hydrothermal evolution of two stages of gold ...€¦ · neumayr under the auspices of the...

Hydrothermal Evolution of Two Stages of Gold Mineralization at the Orogenic New Celebration Gold

Deposit, and Implications for Gold Mineralization within the Kalgoorlie-Kambalda Corridor, Eastern Goldfields

Province, Western Australia

Joanna L Hodge BSc., MSc. (Hons)

University of Auckland, New Zealand

This thesis is presented for the degree of Doctor of Philosophy

of the University of Western Australia

2010

Centre for Exploration Targeting School of Earth and Environment

Supervised by:

Professor Steffen G. Hagemann Professor T. Campbell McCuaig

ACKNOWLEDGEMENTS

3

ACKNOWLEDGEMENTS The idea for this research project was conceived by Steffen Hagemann and Peter

Neumayr under the auspices of the Predictive Mineral Discovery Cooperative Research

Centre (pmd*CRC). When I abandoned my lucrative career to take up this project I had

no idea of the wild ride that was ahead of me. There have been ups and downs, as

always in life, but I don’t regret a single moment of it, and I thank Steffen particularly,

for providing me with the opportunity to have had this experience. Thanks also to Cam

McCuaig who started off as an industry advisor and graduated to co-supervisor.

The pmd*CRC was a wonderful organization to be involved in as a graduate

student, and provided many opportunities for stimulating discussions with researchers

and industry participants from Australia and around the world. I would particularly like

to recognize their financial contributions, both as a provider of research funds, and also

the added support of a supplementary scholarship, which provided funding for interstate

and overseas travel in the pursuit of professional and personal advancement. Thanks

particularly to Helen Clark and Beverley Allen for facilitating this. I would also like to

thank the Education and Training Committee, for investing so much back into the

students, particularly Lucy Chapman, who started out as a colleague and rapidly became

a friend, and Bruce Goleby.

There are a number of people who came to the party with analytical facilities

and words of wisdom for those of us who strayed into geochemistry accidently – Dave

Banks at the University of Leeds, Sarah Gilbert at the University of Tasmania, and

particularly Keith Harris and Garry Davidson for assistance with sulfur isotope analyses

and for always providing a barbie and a beer in Hobart.

On a more personal level, thanks to all my office mates over the last years who

made day-to-day thesis writing a lot more bearable – you have all come and gone and I

ACKNOWLEDGEMENTS

4

am still here…. Thanks to Tansy for coming to Perth and convincing me to move to

Vancouver, and a big hi to all my friends in Vancouver who still keep inviting me out –

even though I turn you down every time – no excuses now! My family have always

believed in my ability to do whatever I turned my hand to, even when some of the

decisions (like this one), caused them to look a little sideways and without their support

I doubt that the last seven and a half years would have seemed achievable. Finally

though, this is for my husband Art, who gave me the motivation and means to submit,

and the incentive to finally be done and move on with our life together.

December 19th, 2010

TABLE OF CONTENTS

5

ACKNOWLEDGEMENTS .................................................................................. 3

ABSTRACT ........................................................................................................ 9

1 CHAPTER ONE: INTRODUCTION ........................................................... 12

1.1 Archean Orogenic Lode Gold Deposits ........................................................... 12 1.1.1 Global Distribution ..................................................................................... 12 1.1.2 Deposit Genesis ........................................................................................... 12 1.1.3 Outstanding Questions ................................................................................ 13

1.2 Thesis Objectives ............................................................................................... 14 1.3 Study Area ......................................................................................................... 15 1.4 Previous Work ................................................................................................... 17

1.4.1 Exploration and Production History............................................................ 17 1.4.2 Research ...................................................................................................... 17

1.5 Research Methods ............................................................................................. 18 1.5.1 Fluid Inclusions ........................................................................................... 18 1.5.2 Sulfur Isotopes ............................................................................................ 19 1.5.3 Mineral Chemistry ...................................................................................... 20

1.6 Thesis Organization .......................................................................................... 20

2 CHAPTER TWO: GEOLOGY OF THE KALGOORLIE TERRANE ........... 23

2.1 Stratigraphy ....................................................................................................... 23 2.2 Deformation ....................................................................................................... 25

2.3 The Boulder-Lefroy Fault Zone ....................................................................... 25 2.4 Distribution and Timing of Gold Mineralization ........................................... 28

3 CHAPTER THREE: GEOLOGY OF THE NEW CELEBRATION GOLD DEPOSIT .......................................................................................................... 30

3.1 Mine Stratigraphy ............................................................................................. 30 3.2 Mine Deformation Events and Regional Correlation .................................... 32 3.3 Gold Mineralization and Hydrothermal Alteration ...................................... 33

3.3.1 Pre-gold and Regional Alteration................................................................ 36 3.3.2 Stage I Gold Mineralization and Related Alteration ................................... 37

3.3.3 Stage II Gold Mineralization and Related Alteration ................................. 37 3.3.4 Post Gold Alteration .................................................................................... 39

3.4 Vein Paragenesis and Petrography ................................................................. 42 3.4.1 Vein Types .................................................................................................. 42 3.4.2 Vein Mineralogy and Textures.................................................................... 42

3.5 Summary ............................................................................................................ 44

4 CHAPTER FOUR: INTEGRATED FLUID STUDY .................................... 46

4.1 Sample Selection, Preparation and Analytical Procedures ........................... 46 4.1.1 Sample Selection and Preparation ............................................................... 46 4.1.2 Microthermometry Procedures ................................................................... 47 4.1.3 Laser Raman Procedures ............................................................................. 48

4.1.4 In Situ Fluid Inclusion Laser Ablation-ICP-MS Procedures ...................... 48

4.2 Fluid Inclusion Petrography ............................................................................ 49 4.2.1 Fluid Inclusion Classifications and Assemblages ....................................... 49

4.2.2 Fluid Inclusion Types .................................................................................. 50

4.3 Relative Timing Constraints ............................................................................ 53 4.4 Microthermometry and Laser Raman Results .............................................. 54

TABLE OF CONTENTS

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4.4.1 Type 1 CH4 Inclusions ................................................................................ 54

4.4.2 Type 2 H2O-CO2 Inclusions ........................................................................ 54 4.4.3 Type III CO2-Rich Inclusions ..................................................................... 60 4.4.4 Type IV H2O-Rich Inclusions ..................................................................... 60 4.4.5 Interpretation of Laser Raman and Microthermometry Results ................. 61 4.4.5.1 Evidence for Fluid Immiscibility ............................................................ 61 4.4.5.2 Trapping Conditions ............................................................................... 63 4.4.5.3 Fluid Mixing ........................................................................................... 67

4.5 LA-ICP-MS Results .......................................................................................... 69 4.5.1 Gold ............................................................................................................. 70 4.5.2 Interpretation of In Situ Laser Ablation ICP-MS Results ........................... 73 4.5.2.1 Potential Fluid Sources ........................................................................... 73

4.6 Comparisons with Other Hydrothermal Systems .......................................... 73

5 CHAPTER FIVE: SULFUR ISOTOPIC COMPOSITION AND MINERAL CHEMISTRY OF SULFIDES, OXIDES AND GOLD ......................................... 78

5.1 Sulfur Isotopic Composition of Pyrite ............................................................. 78 5.1.1 Sample Selection and Analytical Procedure ............................................... 78 5.1.2 Results ......................................................................................................... 79 5.1.3 Interpretation of Results .............................................................................. 83 5.1.3.1 Sulfur Sources ......................................................................................... 83 5.1.3.2 Ore Forming Processes and their Influence on the Sulfur Isotopic Composition of Pyrite ............................................................................................. 84

5.1.4 Summary ..................................................................................................... 87 5.1.5 Comparisons with other Hydrothermal Mineral Systems ........................... 88 5.1.5.1 Orogenic Lode Gold Deposits ................................................................. 88 5.1.5.1.1 Eastern Goldfields Province ................................................................ 89 5.1.5.1.2 Global Examples ................................................................................. 90 5.1.5.2 Other Gold Mineral Systems ................................................................... 91

5.2 Sulfide, Oxide and Gold Mineral Chemistry .................................................. 92 5.2.1 Sample Selection, Preparation and Analytical Procedure ........................... 92 5.2.2 Results ......................................................................................................... 93 5.2.2.1 Pyrite ....................................................................................................... 93 5.2.2.2 Fe-oxides ................................................................................................. 94

5.2.2.3 Gold ......................................................................................................... 95 5.2.3 Interpretation of Mineral Chemistry ........................................................... 96 5.2.3.1 Tellurium ................................................................................................. 96

5.2.3.2 Ore Forming Processes and Mineral Chemistry ..................................... 98 5.2.4 Comparisons with other Hydrothermal Gold Mineral Systems .................. 99

6 CHAPTER SIX: HYDROTHERMAL FLUID MODEL FOR THE NEW CELEBRATION SYSTEM .............................................................................. 101

6.1 Ore Forming Processes ................................................................................... 101 6.1.1 Wall Rock Reaction .................................................................................. 101 6.1.2 Phase Immiscibility ................................................................................... 102

6.1.3 Fluid Mixing ............................................................................................. 103

6.2 Constraints on Fluid and Metal Sources ....................................................... 104 6.3 Integrated Model for the Evolution of the New Celebration Gold Mineral System within the BLFZ ......................................................................................... 108

6.3.1 Early Evolution (D1-D2)........................................................................... 108 6.3.2 Early D3NC ................................................................................................ 109

TABLE OF CONTENTS

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6.3.3 Stage I Gold Mineralization (D3NC) .......................................................... 110

6.3.4 Stage II Gold Mineralization (Late D3NC-Early D4NC) ............................. 111 6.3.5 Post-gold evolution (>D4) ........................................................................ 111

6.4 Comparisons with other Orogenic Lode Gold Systems ............................... 112 6.4.1 Host Rocks and their Role in Gold Precipitation ...................................... 112 6.4.2 Methane-rich and Highly Saline Aqueous Fluids ..................................... 113 6.4.3 Cation Ratios and Metal Concentrations in Hydrothermal Fluids ............ 118 6.4.4 Sulfur Isotopes .......................................................................................... 121 6.4.5 Structural Setting ....................................................................................... 123

6.5 Key factors in the Location of the New Celebration Deposit ...................... 123 6.6 Outstanding Questions ................................................................................... 125

6.6.1 Fluid and Metal Source ............................................................................. 125

6.6.2 Timing of mineralization........................................................................... 126

6.7 Summary .......................................................................................................... 127

7 CHAPTER SEVEN: PROTRACTED GOLD MINERALIZATION IN THE KALGOORLIE-KAMBALDA CORRIDOR AND ITS RELATIONSHIP TO THE BOULDER-LEFROY FAULT ZONE, EASTERN GOLDFIELDS PROVINCE, WESTERN AUSTRALIA ................................................................................ 128

ABSTRACT ............................................................................................................. 128 1. INTRODUCTION ........................................................................................... 129 2. REGIONAL GEOLOGY ............................................................................... 131

2.1 The Boulder-Lefroy Fault Zone ................................................................ 135

3. HISTORY OF GOLD MINERALIZATION IN THE KALGOORLIE-KAMBALDA CORRIDOR .................................................................................... 135 4. GEOLOGY OF THE MAJOR GOLD CAMPS IN THE KALGOORLIE-KAMBALDA CORRIDOR .................................................................................... 137

4.1 Deposit Geology ........................................................................................ 137 4.2 Deformation and Timing of Gold Mineralization in the Kalgoorlie-Kambalda Corridor ............................................................................................... 141 4.3 Hydrothermal Alteration Mineralogy Spatially and/or Temporally Related to Gold Mineralization .......................................................................................... 143 4.4 Hydrothermal Fluid Chemistry Associated with Gold Mineral Systems in the Kalgoorlie-Kambalda Corridor ...................................................................... 145 4.5 Carbon, Oxygen and Hydrogen Stable Isotopes ....................................... 149 4.6 Sulfur Isotopic Composition and Comparison with Previous Studies ...... 150

4.7 Mineral Chemistry of Sulfides, Oxides and Gold Associated with Gold Mineral Systems in the Kalgoorlie-Kambalda Corridor ...................................... 155

5. EVOLUTION OF THE BOULDER-LEFROY FAULT ZONE AND ITS POTENTIAL ROLE IN THE LOCATION OF GOLD MINERALIZATION IN THE KALGOORLIE-KAMBALDA CORRIDOR ............................................. 160

5.1 D1- early D2 (>2675 – 2670) ................................................................... 160 5.2 Late D2 (2670 – 2660) .............................................................................. 164 5.3 D3 (2660-2647 Ma) -D4 (<2640 Ma) Deformation ................................. 165

5.4 Post-D4 ..................................................................................................... 168

6. DISCUSSION .................................................................................................. 177 6.1 Geochemistry............................................................................................. 177 6.2 Timing ....................................................................................................... 178

7. CONCLUSIONS ............................................................................................. 181 ACKNOWLEDGEMENTS.................................................................................... 183

TABLE OF CONTENTS

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8 CHAPTER EIGHT: CONCLUSIONS ....................................................... 184

8.1 New Celebration Hydrothermal Fluid System ............................................. 184 8.1.1 Gold Mineralization .................................................................................. 185 8.1.2 Hydrothermal Evolution............................................................................ 187

8.2 Regional Hydrothermal Fluid System ........................................................... 188 8.3 Exploration Implications ................................................................................ 190 8.4 Future Work .................................................................................................... 190

REFERENCES ............................................................................................... 192

APPENDIX 1: “The New Celebration Gold Deposits: P-T-X Fluid Evolution and Two Stages of Gold Mineralization within the Crustal-scale Boulder-Lefroy Shear Zone, Yilgarn Craton, Western Australia” ............................ 215

APPENDIX 2 Sample Data ............................................................................ 272

APPENDIX 3 Petrographic Descriptions ..................................................... 275

APPENDIX 4 Fluid Inclusion Microthermometry ........................................ 302

APPENDIX 5 Laser Raman Analyses .......................................................... 307

APPENDIX 6 LA-ICP-MS Fluid Inclusion Analyses .................................... 309

APPENDIX 7 Sulfur Isotopic Analyses ........................................................ 320

APPENDIX 8 LA-ICP-MS Mineral Chemistry ............................................... 325

APPENDIX 9 Whole-Rock Geochemistry – Methodology And Results ... 382

ABSTRACT

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ABSTRACT The Archean orogenic New Celebration gold deposit, located in the Kalgoorlie

Terrane of the Eastern Goldfields Province, Western Australia, is hosted within the

western segment of the first-order Boulder Lefroy fault zone (BLFZ). This setting

contrasts with the majority of orogenic lode gold deposits worldwide, which are

typically located in higher order splays, and as such, the New Celebration deposit

provides a unique opportunity to study the hydrothermal, structural, alteration and fluid

characteristics of a first-order crustal scale shear zone. Fluid inclusion, sulfur isotope

and mineral chemistry were used to reconstruct the evolution of hydrothermal fluids

within the BLFZ. Vein petrography, fluid inclusion microthermometry and laser

ablation-inductively coupled plasma-mass spectrometry microanalysis (LA-ICP-MS) of

single fluid inclusions, in addition to laser ablation sulfide sulfur isotope analyses and

LA-ICP-MS mineral chemistry were combined to determine the pressure-temperature-

composition evolution of the New Celebration gold deposit.

At New Celebration, gold mineralization took place in two stages: Stage I,

which is related to ductile, sinistral oblique slip fault movement and Stage II, which is

related to brittle-ductile and brittle strike-slip fault movement. Type 2 quartz and quartz-

calcite shear and extension veins concomitant with Stage I gold mineralization contain

pseudo-secondary 2- and 3-phase aqueous-carbonic (10 ± 1 to 33 ± 13 mole % CO2)

inclusions with salinities between 2 and 8 equiv. wt. percent NaCl, which were trapped

between 330° and 390° C and 3.2 and 4.0 kbars. Mixed aqueous-carbonic inclusions (16

± 3to 53 ± 28 mole % CO2) and aqueous>>carbonic fluid (<3 mole % CO2) inclusions

with variable phase ratios and salinities of 1.9 ± 1.1to 8.7 ± 2.6 equiv. wt. percent NaCl

in type 3 quartz-pyrite±sericite±calcite veins and quartz-calcite alteration associated

with Stage II gold mineralization were trapped between 280° and 320° C and 0.8 to 3.2

kbars. Coexisting liquid- and vapor-rich inclusions within the same trail or cluster

indicate these inclusions were trapped during phase separation. Secondary high-salinity

(18.4 to 23.3 equiv. wt. % NaCl) aqueous inclusions, and metane inclusion, which post-

dated gold mineralization, were trapped in type 2 and type 3 veins between 100° C and

180° C and pressures below 1 kbar.

Single inclusion laser ablation inductively coupled plasma mass spectrometry

analyses on aqueous and aqueous-carbonic inclusions indicate that the Stage I gold

related fluids were characteristically Na>Ca>K> Mg (K/Ca <1) whereas Stage II fluids

ABSTRACT

10

are Na>Mg>K>>Ca (K/Ca >1) and contained higher concentrations of, Pb, Zn, As, and

W than Stage I fluids. Average Au concentrations from both Stage I and Stage II-related

aqueous-carbonic inclusions returned values around 5 parts per million (ppm) although

individual inclusions contained up to 51 ppm. Variations in metal ratios and elemental

concentrations, in addition to K/Ca ratios potentially indicate different fluid sources for

each mineralizing event and suggest that a switch occurred in fluid and/or metal sources

between Stage I and Stage II.

Laser ablation inductively coupled plasma mass spectrometry analyses indicate

that New Celebration ore stage pyrites ubiquitously contain Ni and Co. Additionally,

Stage II pyrites contain Ti, W, Pb, Zn and Cr. Pyrites from both mineralization stages

contain trace Au-Ag±Pb tellurides. Gold grains from both Stages I and II contain trace

Te. Sulfur δ34S isotope values in ore-stage pyrite range between -7.6 per mil and +3.8

per mil in Stage I mineralization, and between -10.6 per mil and -3.2 per mil in Stage II

mineralization. These values are predominantly within the documented range for

orogenic lode gold deposits worldwide, although the negative values are amongst the

most negative values reported. The isotopic composition of the Stage I ore stage pyrites

likely reflect the redox state of the ore-forming fluids, whereas the negative values of

Stage II ore-related pyrite and the spread of observed values are attributed to fluid

oxidation during phase separation.

Pressure-temperature estimates describe an anticlockwise path and indicate that

Stage I gold mineralization occurred at temperatures and pressures similar to peak

regional metamorphism, whereas Stage II gold formed at lower temperatures and

fluctuating pressures, likely during a period of uplift, erosion and fault movement.

Replacement of magnetite by pyrite indicates that sulfidation reactions with Fe-oxides

were the main cause of gold mineralization in both mineralizing stages and the sole

cause of gold mineralization during Stage I. Fluid inclusion evidence suggests that

phase separation contributed to Stage II gold formation. The variety of fluids recorded

within the BLFZ and their diverse formation conditions suggest that the BLFZ was the

main conduit for gold-related and unrelated fluids at New Celebration over a protracted

period. Furthermore, it appears that during the evolution of the BLFZ it tapped at least

two geochemically distinct crustal fluid reservoirs, which led to the development of two

gold mineralization stages at New Celebration with differing geochemical

characteristics.

ABSTRACT

11

Regional models propose that a number of large gold camps, including the

Golden Mile to the north of New Celebration and St Ives to the south, are spatially,

temporally and genetically related to each other and the BLFZ. Integration of the data

collected during this study on New Celebration, with new geochemical data on ore-

stage sulfides from the Golden Mile and St Ives deposits and data collected over the last

100 years from these three gold camps indicate that at the Golden Mile, Fimiston and

Oroya lodes are unrelated to either the BLFZ or to other gold mineralization events in

the Kalgoorlie-Kambalda corridor. Their unique pyrite (As, Te, Sb-rich) composition,

association with abundant telluride mineralization, and V-rich roscoelite alteration, not

observed elsewhere in the corridor, suggests a link to alkalic magmatism and formation

at temperatures below 300° C at crustal depths less than 6 km. Similarities in sulfide

geochemistry between the St Ives and New Celebration deposits, in conjunction with

hydrothermal fluid and structural characteristics identified by other researchers, suggest

that gold mineralizing events at New Celebration and St Ives are genetically related.

Furthermore, structural relationships between both these camps and the BLFZ indicate

that mineralization at both is related to the formation and evolution of the BLFZ. Recent

work on the Golden Mile proposes that gold mineralization took place during D1-D2

deformation, i.e. earlier than the commonly proposed D3 event, and structural

interpretations of the BLFZ indicate that the fault system was not developed at that

time. Results of this study, interpreted with recently published conclusions on the

timing of gold mineralization at the Golden Mile, indicate that gold formation was

unrelated either to the BLFZ or to mineralization at New Celebration or St Ives.

CHAPTER ONE: INTRODUCTION

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1 CHAPTER ONE: INTRODUCTION

1.1 Archean Orogenic Lode Gold Deposits

1.1.1 Global Distribution

Orogenic lode gold deposits are common to Archean granitoid-greenstone belts

world wide, and are amongst the largest gold deposits found anywhere on Earth, with

world class examples containing in excess of 100 tonnes of gold (Groves and Foster,

1993; Robert and Poulsen, 1997). Most Archean cratons host these types of deposits,

which collectively contribute approximately one fifth of the world’s total gold

production (Roberts, 1988). Some of the world’s largest gold deposits are Archean

orogenic lode gold deposits, including the Golden Mile (Western Australia), Hollinger-

McIntyre (Canada) and Kolar (India). Western Australia has produced over 5000 tonnes

of gold since the early 1890’s (data to December 2001, Department of Minerals and

Energy), almost all of which has been from Archean orogenic lode gold deposits, with

the world class Golden Mile in Kalgoorlie (>1,400t, Hagemann and Cassidy, 2000)

contributing over 30% of the state’s total production.

1.1.2 Deposit Genesis

Archean orogenic lode gold deposits comprise a group of genetically, temporally

and spatially related gold-only deposits commonly associated with metamorphic

terranes (Groves et al., 1998). They formed along convergent margins during terrane

accretion, translation or collision related to subduction or lithospheric delamination, and

traditional genetic models place them late in the deformational-metamorphic-magmatic

history of evolving volcano-plutonic terranes (Groves et al., 2000; Hagemann and

Cassidy, 2000). Gold mineralization has typically been inferred to take place late in the

deformation history of the orogen, usually synchronous with, or just post-dating, peak

metamorphism (Colvine et al., 1988; Clark et al., 1989; Groves et al., 1989; Hodgson,

1993; Kerrich and Cassidy, 1994; McCuaig and Kerrich, 1998; Ridley and Mengler,

2000) although recent models for some Yilgarn deposits, e.g. Golden Mile (Bateman et

al., 2001; Bateman and Hagemann, 2004) and Jundee (Yeats et al., 2001; Baggott et al.,

in press), propose an earlier timing for gold mineralization. Any rock type may host

gold mineralization (Hodgson, 1993), although in the Yilgarn and Pilbara cratons of

Western Australia iron-rich mafic and ultramafic lithologies are the dominant hosts

(Groves, 1990). Gold deposits are predominantly restricted to rocks metamorphosed to


13

greenschist facies (Goldfarb et al., 2005). Deposits are structurally controlled, with

faults, shear zones, folds and competency contrasts between different rock types

important at both regional, camp and deposit scales (Eisenlohr et al., 1989; Groves et

al., 1990), and some of the most gold-rich camps show a common association with fold

hinges and anticlinal structures (Goldfarb et al., 2005). Gold mineralization may be

vein- or wall rock- hosted (Groves, 1990; Hagemann and Cassidy, 2000; Eilu and

Groves, 2001). Deposits display characteristic chlorite-calcite±biotite (<500 °C) and

amphibole-biotite-calcite±epidote (500-700 °C) alteration assemblages (Mueller and

Groves, 1991) and typically formed from low to moderate salinity aqueous-carbonic

fluids (Mikucki and Groves, 1990; Ridley and Diamond, 2000), which transport gold

(but not other metals) as a bisulfide complex (Seward, 1973, 1984; Benning and

Seward, 1996). Local variations generally reflect formation at varying crustal levels

(Groves, 1993; Gebre-Mariam et al., 1995), differences in host rock type, metamorphic

grade, and P-T conditions of formation (Colvine, 1989; Hagemann and Cassidy, 2000;

Eilu and Groves, 2001) and multiple depositional events over protracted time periods

(Robert and Poulsen, 1997; Groves et al., 2003).

Orogenic lode gold deposits as defined by Groves et al. (1998) include those

categorized as mesothermal (Nesbitt et al., 1986) and are classified according to ore

associations (gold only), host sequences (greenstone-hosted, slate-belt style, turbidite-

hosted), form (lode, quartz-carbonate vein, disseminated) or specific location (Mother-

lode style). They are additionally classified according to their inferred formation depth

as epizonal (<6km), mesozonal (6-12km) or hypozonal (>12km) (Gebre-Mariam et al.,

1995; Groves et al., 1998).

1.1.3 Outstanding Questions

There has been much research undertaken on Archean orogenic lode gold

deposits in the last thirty years, however, a number of questions regarding their genesis

remain outstanding. It is particularly noteworthy that despite almost 30 years of research

into orogenic lode gold deposits, the problem of fluid and/or metal source remains

equivocal. Other significant questions are those regarding the nature, source(s) and

pressure-temperature-composition-timing (P-T-X-t) characteristics of pre- and post-gold

fluids, which constrain the tectonic and fluid evolution of the entire hydrothermal

system, and the role that crustal-scale fault systems, which are spatially associated with

Archean orogenic lode gold systems worldwide, play in mineralization. Some of these

questions have been addressed and partially resolved by recent work, including research


14

focused on the structure (Robert, 1989; Wilkinson et al., 1999), timing of mineralization

(Robert, 1990; Neumayr et al., 2000), hydrothermal fluid evolution (Neumayr and

Hagemann, 2002) and tectonic evolution (Neumayr et al., 2007) of the Cadillac

Tectonic Zone in the Abitibi greenstone belt.

1.2 Thesis Objectives

Archean orogenic lode-gold deposits worldwide typically show a close spatial

association with first-order, crustal-scale shear zones (Eisenlohr et al., 1989; Neumayr

et al., 2000), such as the Boulder-Lefroy (Western Australia) or the Destor-Porcupine

(Ontario) fault zones. At a camp- to deposit- scale, however, second- and third-order

splays host the majority of world class (>100t Au) orogenic lode gold deposits

(Eisenlohr et al., 1989; Groves, 1990). Much research into the fluid chemistry and P-T-

X-t evolution of hydrothermal fluids in the gold-endowed second- and third-order fault

systems has been undertaken, however, first-order faults have largely been ignored. This

is predominantly because most first-order fault systems are barren and research has

focused on mineralized lower-order faults adjacent to the main trans-crustal faults, but

is also due to the poor exposure of first-order faults. Recent research on first-order

systems has focused on the structure (Robert, 1989; Wilkinson et al., 1999; Neumayr

and Hagemann, 2002), timing of mineralization (Robert, 1990; Neumayr et al., 2000)

and hydrothermal fluid composition (Neumayr and Hagemann, 2002) on the Cadillac

Tectonic Zone in the Abitibi greenstone belt. More recently, researchers under the

auspices of the Predictive Mineral Discovery Cooperative Research Centre (pmd*CRC)

have worked on deposits associated with the Boulder Lefroy Fault Zone in the New

Celebration-Kambalda corridor, including Honours projects at New Celebration, and at

the Junction deposit in Kambalda and an integrated fluid and alteration study at St Ives.

The Boulder-Lefroy fault zone (BLFZ) is an interpreted, first-order crustal-scale

fault zone located in the Eastern Goldfields Province of the Yilgarn craton (Swager,

1989). It is spatially correlated with the Golden Mile (>1400 t Au) and St Ives (>200 t

Au) gold camps, both of which are hosted in adjacent second- and third-order splays.

The BLFZ also hosts the New Celebration gold deposit (>150 t Au). As orogenic gold

deposits hosted in first-order fault systems are rare, the New Celebration gold deposit

provides a unique opportunity to study the P-T-X-t-d evolution of hydrothermal fluids

in such a system, and evaluate the role regional scale structures play in focusing

mineralizing and non-mineralizing fluids.


15

The aims of this PhD thesis are to: (1) document the fluid evolution in pressure-

temperature-composition (P-T-X) space of the western segment of the Boulder Lefroy

Fault Zone at the New Celebration gold deposit; (2) establish a paleohydrothermal fluid

model for the New Celebration gold deposit; (3) characterize the metal content of

mineralizing and non mineralizing fluids at the New Celebration gold deposit; (4)

evaluate potential fluid source(s) for both the mineralizing and non-mineralizing fluids;

and (5) determine the major and trace element composition of ore-related sulfides,

oxides and gold.; It also aims to (6) establish a regional hydrothermal fluid model for

the Kalgoorlie-Kambalda region, and evaluate potential links between gold mineralizing

events along the extent of the BLFZ through the integration and interpretation of data

available from the literature, unpublished sources and data collected during this research

project.

1.3 Study Area

The New Celebration gold deposit is located in the Eastern Goldfields province

of the Yilgarn craton, Western Australia, approximately 30km south of Kalgoorlie

(Figure 1.1). Geographically it is located at Latitude -31.03, Longitude 121.60 on the

Geological Survey of Western Australia Widgiemooltha (SH 51-14) 1:250 000 and

Lake Lefroy (3235) 1:100,000 map sheets. Access to the deposit is via the Kalgoorlie-

Kambalda Highway (94) and mine haul roads. Pit wall failure in the now-closed open

pit restricts access to much of the pit; however, abundant drill core is available.

The Kalgoorlie and Kambalda gold camps are located to the north and south of

New Celebration deposits, along the strike of the BLFZ. Geographically, the Kalgoorlie

deposits are located at Latitude -30.76, Longitude 121.51 on the Kurnalpi (SH51-10)

1:250,000 and Kanowna 3236 (1:100,000 map sheets. The Kambalda deposits are

located at Latitude -31.29, Longitude 121.74 on the Widgiemooltha (SH51-14)

1:250,000 and Lake Lefroy (3235) 1:100,000 map sheets. Samples and unpublished data

from these deposits were obtained from Steffen Hagemann and Louis Gauthier

(Kalgoorlie samples) and Klaus Petersen (Kambalda samples).


16

Figure 1.1 Simplified geological map of the Kalgoorlie-Kambalda region highlighting

the spatial correlation between the Boulder Lefroy fault zone and the Kalgoorlie

(Golden Mile), New Celebration and Kambalda (St Ives) deposits.


17

1.4 Previous Work

1.4.1 Exploration and Production History

Gold was first discovered in the New Celebration area in 1890 (Gresham, 1991)

but it was not until 1919 that significant discoveries, such as Celebration, Dawns Hope,

White Hope, Villiers Bretonneux, Jubilee and Triumph, named predominantly to reflect

the post-World War I social climate, were made (Norris, 1990; Copeland, 1998). The

town of Celebration City was established adjacent to the Celebration mine and serviced

a number of mining operations. Mining declined in the mid 1920’s, due to a fixed gold

price, lack of water and manpower shortages (Norris, 1990; Copeland, 1998).

In 1980, Hampton Areas Australia Limited (HAAL) and Newmont Australia Ltd

signed the Location 50 Joint Venture agreement, although HAAL subsequently excised

the Jubilee lease from the joint venture. Soil sampling, RAB and RC drilling delineated

the Hampton-Boulder deposit for the JV partners (Norris, 1990) and the Jubilee deposit

for HAAL (Copeland, 1998). Between 1986 and 1997, the Hampton-Boulder deposit

produced 7.4 million tonnes at 2.34 g/t Au for 557,000 ounces from the open pit and

1.01 million tonnes at 6.38 g/t Au for 207,000 ounces from underground. The Jubilee

pit produced 10.3 million tonnes at 2.09 g/t Au for 694,000 ounces in its ten years of

operation between 1987 and 1997 (Newcrest Mining Limited Internal Report, 2000). In

2001, Harmony Gold Australia Pty Ltd acquired and amalgamated the entire tenement

holdings previously held by separate owners. Dioro Exploration NL took over the

deposits in December 2007.

1.4.2 Research

A number of workers have studied various aspects of the New Celebration gold

deposits. Previous workers have focused on the structural (Dielemans, 2000) and

lithological controls (Williams, 1994) of Southern Ore Zone mineralization within the

Hampton-Boulder segment of the deposit, and on the structural and lithological controls

within the Jubilee segment of the deposit (Williams, 1991). More recently, Nichols

(2003) and Nichols et al. (in revision) evaluated the structural controls, hydrothermal

alteration and timing of mineralization of the entire New Celebration gold system.

Weinberg et al. (2005) established a kinematic history for the Boulder-Lefroy shear

zone and evaluated the controls on associated gold mineralization along its entire

length. Hodkiewicz (2003) studied the sulfur stable isotopic composition of ore-related

sulfides from New Celebration as part of a much larger regional-scale study on the


18

physical and chemical processes within orogenic lode gold deposits of the Yilgarn

craton. A number of authors have published summaries of various aspects of the New

Celebration deposits, including Norris (1990) who discussed all aspects of the

Hampton-Boulder deposits, Copeland (1998), who summarized the Jubilee deposits,

and Witt (1993a) who included the New Celebration deposits within a wider framework

of deposits between Kalgoorlie and Kambalda.

1.5 Research Methods

New Celebration samples selected for analysis were taken from the Hampton-

Boulder and Jubilee open pits, diamond drill core, and samples collected by Nichols

(2003) and archived in the Edward de Courcy Clarke Museum at the University of

Western Australia. Steffen Hagemann and Louis Gauthier provided Kalgoorlie (Golden

Mile) samples; Klaus Petersen provided Kambalda samples from the St Ives deposits.

Polished thin sections for petrography and double polished thick sections for fluid

inclusion microthermometry, laser Raman and LA-ICP-MS analysis were made at the

University of Western Australia. Single polished thick sections for sulfur isotope

analysis were prepared at the University of Tasmania or by Pontifex Associates

(Adelaide). Polished block mounts for LA-ICP-MS mineral chemistry were prepared at

the University of Tasmania. Acme Analytical Laboratories Ltd in Vancouver, Canada,

crushed and analyzed New Celebration samples for whole rock major and trace element

geochemistry. The author completed transmitted and reflected light petrography, and

fluid inclusion microthermometry at the University of Western Australia, Laser Raman

analyses at Geoscience Australia in Canberra, sulfur isotope analyses and LA-ICP-MS

(laser ablation inductively coupled plasma mass spectroscopy) mineral chemistry

analyses at the University of Tasmania and single fluid inclusion LA-ICP-MS analyses

at the University of Leeds. This study builds on the excellent mapping and structural

work completed by Nichols (2003) and Nichols et al. (submitted) as part of a BSc.

(Hons) project completed at the University of Western Australia.

1.5.1 Fluid Inclusions

Fluid inclusions provide the only direct evidence of the fluids ascending through

the Earth’s crust and impart valuable information on the composition of ore forming

(and other) fluids, in addition to constraining formation temperatures and pressures.

Detailed petrography on well-constrained samples, in conjunction with good


19

documentation of mineral and fluid paragenesis is therefore critical when interpreting

the data.

The New Celebration samples selected for analysis in this study were chosen to

reflect the different host rocks, deformation events and mineralization events and styles

established within the deposit (Nichols, 2003). Quartz±calcite veins from these samples

were categorized according to their mode of occurrence, mineral composition and

petrographic features, and correlated to the local deformation sequence established by

Nichols (2003). Fluid inclusions from these vein samples were examined

petrographically to identify different inclusion populations and types, reflecting pre-,

syn and post-mineralization fluids, whose evaluation is critical to establishing the

hydrothermal and tectonic history of the fault. Fluid inclusion data from the Golden

Mile and Kambalda deposits were obtained from the literature (Scantlebury, 1983;

Phillips, 1986; Ho, 1987; Clark et al., 1989; Clout, 1989; Ho et al., 1990; Mernagh,

1996; Neumayr et al., 2004; Petersen et al., 2005) or unpublished data (Petersen et al.,

submitted; K. Petersen, pers. comm. 2007)

1.5.2 Sulfur Isotopes

Gold in orogenic lode gold deposits typically precipitates in equilibrium with

sulfide minerals and is transported in the hydrothermal fluid as a bisulfide complex

(Seward, 1973; Mikucki, 1998). Sulfide sulfur isotopic composition is determined by

the source fluid composition and by physicochemical parameters at the depositional site,

such as pH, temperature and pressure (Ohmoto and Rye, 1979). Sulfur isotopes,

therefore, provide vital evidence about the oxidation state of ore fluid, which has

implications for gold solubility and the ability of the fluid to transport and precipitate

gold, and may provide evidence for fluid source or ore depositional processes.

The New Celebration samples were chosen to reflect the two gold mineralizing

events and four gold mineralizing styles observed within the deposit. Thirty-seven

Golden Mile samples were selected to represent syn-volcanic sulfides, different

mineralization styles (Fimiston and Oroya), different lode systems (East, West and

Aberdare), different chronological events within a single lode system (Fimiston Stages

I-IV), and shallow vs. deep gold mineralization (Hagemann et al., 1999). The Kambalda

samples represent different hydrothermal alteration fluid systems from within the

Conqueror and Revenge deposits at St Ives. The results of this study are compared with

existing data on sulfides from the Golden Mile (Lambert et al., 1984; Clout, 1989;


20

Hagemann et al., 1999; Bateman et al., 2001; Bateman and Hagemann, 2004), New

Celebration (Hodkiewicz, 2003; Hodkiewicz et al., 2009; Hodge et al., in revision) and

St Ives (Palin and Xu, 2000; Hodkiewicz, 2003; Walshe et al., 2006) .

1.5.3 Mineral Chemistry

Sulfide, oxide and gold mineral chemistry can potentially be a sensitive indicator

of the ore fluid oxidation state, and provide valuable information on the ore fluid

chemistry. Pyrite, pyrrhotite, magnetite, ilmenite and gold from New Celebration,

Golden Mile and St Ives deposits were analyzed by LA-ICP-MS (laser ablation

inductively coupled mass spectrometry) to evaluate potential links between mineralizing

and hydrothermal alteration events at all three camps, and in the case of New

Celebration, to determine similarities between fluid chemistry (as determined by LA-

ICP-MS of individual fluid inclusions) and ore-bearing pyrite and gold grains.

1.6 Thesis Organization

This thesis was originally planned to be submitted as a series of three

publications to be published in earth science journals; however, a change in

organization partway through the research process necessitated a change in the thesis

organization. This thesis is therefore presented as a series of chapters (2 to 6, 8), and a

stand-alone paper (chapter 7), which includes a separate abstract. The organization of

the PhD thesis is compatible with the University of Western Australia rules for

submission of a PhD thesis.

Chapters 2 to 6 form the basis for a paper entitled “The New Celebration Gold

Deposits: P-T-X Fluid Evolution and Two Stages of Gold Mineralization within the

Crustal-scale Boulder-Lefroy Shear Zone, Yilgarn Craton, Western Australia” which

was submitted for publication in Economic Geology and is currently in revision. This

paper is presented as Appendix 1. The paper was co-authored by Steffen G. Hagemann,

Peter Neumayr, Garry Davidson and David Banks. The first author conducted all thin

section and polished section petrography, fluid inclusion petrography and

microthermometry, laser Raman analyses, single fluid inclusion laser ablation-ICP-MS

analyses, in situ sulfur isotope analyses and laser ablation-ICP-MS mineral chemistry

analyses, and wrote the first draft of the paper. Co-authors S. Hagemann, P. Neumayr

and G. Davidson read drafts of this paper and provided editorial comments. Co-authors

G. Davidson and D. Banks provided access to analytical facilities at the University of

Tasmania and the University of Leeds, respectively.


21

Chapter 7 comprises a single paper, entitled “Protracted Gold Mineralization in

the Kalgoorlie-Kambalda Corridor and its Relationship to the Boulder-Lefroy Fault

Zone, Eastern Goldfields Province, Western Australia”, which was prepared for

submission to Ore Geology Reviews, and as such is presented as a paper, including a

separate abstract. The first author conducted the laser ablation ICP-MS mineral

chemistry analyses, the in situ sulfur isotope analyses not referenced to other studies,

literature research, and wrote the first draft of the paper. The co-authors S. Hagemann,

T.C. McCuaig and P. Neumayr read drafts of this paper and made scientific and

editorial comments.

Chapter 8 presents the conclusions of the entire research project and

encompasses the conclusions from chapters 2-6 and chapter 7.

Chapter 2 describes the regional geological setting of the Yilgarn craton,

Norseman-Wiluna belt and the Kambalda Domain. Chapter 3 presents the geology of

the New Celebration deposits including the structural setting of the mine and its

correlation with regional events, lithostratigraphy, gold mineralization, hydrothermal

alteration and vein paragenesis. This chapter predominantly presents the work of

previous researchers, particularly that of Nichols (2003), whose BSc. (Hons) thesis on

the structural control, hydrothermal alteration and relative timing of the New

Celebration gold deposit provided the deposit framework upon which this research

project was developed. All data and interpretations presented on quartz vein

mineralogy, and the paragenetic sequence is the candidates own, except where

otherwise referenced. Chapter 4 describes the results of fluid inclusion petrography,

microthermometry, Laser Raman and LA-ICP-MS geochemical analyses, evaluates the

trapping conditions of the different fluids, and the tectonic implications of these results

and interpretations. Chapter 5 presents the results of sulfide sulfur isotope and sulfide,

oxide and gold geochemistry analyses, and their implications for potential fluid sources

and ore forming processes. Chapter 6 discusses the New Celebration hydrothermal

system and proposes an integrated hydrothermal fluid model for the Boulder Lefroy

Fault Zone at New Celebration. Chapter 7 compiles available published and

unpublished fluid inclusion, hydrothermal alteration and radiogenic and stable isotope

data on the Kalgoorlie and Kambalda gold camps, and presents new sulfide sulfur

isotopic data and sulfide, oxide and gold LA-ICP-MS mineral chemistry analyses

collected during this study. This forms the basis for an integrated hydrothermal fluid

model for the Kalgoorlie-Kambalda area and evaluates the role of the Boulder Lefroy


22

Fault Zone in facilitating the flow of metals and fluids to the spatially associated world-

class gold deposits within the Kalgoorlie-Kambalda corridor. Chapter 8 summarizes the

main conclusions of this research, and discusses the potential exploration implications

in addition to possible future work.

CHAPTER TWO: GEOLOGY OF THE KALGOORLIE TERRANE

23

2 CHAPTER TWO: GEOLOGY OF THE KALGOORLIE TERRANE

2.1 Stratigraphy

The Eastern Goldfields Province (EGP) orogenic belt is located on the eastern

margin of the Yilgarn craton (Fig. 2.1) and consists of six stratigraphically and

structurally distinct late Archean (Swager et al., 1992) terranes – Kalgoorlie, Kurnalpi,

Gindalbie, Edjudina, Laverton and Norseman. The Kalgoorlie Terrane is the best

defined terrane of the EGP (Swager et al., 1995) and is a 6-9 kilometer thick, elongate,

NNW trending volcano-sedimentary sequence, bounded to the east and west by wide

(up to 1km) anastamosing shear zones (Swager, 1997). The regionally extensive

volcano-sedimentary greenstone sequence comprises a mafic-ultramafic volcanic

sequence overlain by felsic volcanic and volcaniclastic rocks and intruded by a number

of mafic-ultramafic and granitoid suites. The oldest unit in the Kalgoorlie Terrane is the

Lunnon Basalt, a >200 meter-thick thick pillowed tholeiitic unit with thin interflow

sedimentary rocks. Overlying the Lunnon Basalt is an 800-1200 meter-thick

serpentinized komatiite sequence (named Hannans Lake Serpentinite in the north,

Kambalda Komatiite in the south), which grades upwards into high-Mg basalt. The

Devon Consols basalt (60-100 meter-thick) and Paringa basalt (up to 1500 meter-thick),

both high-Mg variolitic, pillowed basalt lavas, overly the komatiites. The Kapai slate, a

10 meter-thick sulfidic unit and distinctive marker bed throughout the region, separates

the two basalts. The Black Flag Group overlies the mafic volcanic package and

comprises a 1km thick sequence of upwards-coarsening volcano-sedimentary sequence

of black shales, felsic volcaniclastic sandstones, conglomerates and felsic intrusive

rocks. Differentiated tholeiitic mafic sills intrude the volcano-sedimentary sequence and

in Kalgoorlie host most of the gold. The youngest exposed rocks comprise coarse clastic

basins, which unconformably overlie the greenstone sequence and commonly bury

major boundary faults (Swager, 1997). Regionally the terrane is metamorphosed to

upper greenschist facies, with locally higher metamorphic grades (up to amphibolite

facies) recorded along the margins of, and adjacent to, granitoid plutons (Witt, 1991).

The New Celebration deposits mark the transition between lower- to middle-greenschist

facies metamorphism to the north at Kalgoorlie and upper-greenschist facies

metamorphism at St Ives, to the south (Witt and Vanderhor, 1998).


24

Figure 2.1 Geological map of the Yilgarn Craton showing the Eastern Goldfields Province, the location of major gold camps and deposits, the location of the New Celebration, Golden Mile (Kalgoorlie) and St Ives (Kambalda) gold camps, and the terranes of the Eastern Goldfields Province. Modified from Bateman and Hagemann (2004). K = Kalgoorlie Terrane, U = Kurnalpi Terrane, G = Gindalbie Terrane, E = Edjudina Terrane, L = Laverton Terrane, N = Norseman Terrane, BLFZ = Boulder Lefroy Fault Zone.


25

2.2 Deformation

The characteristic NNW-trending tectonic grain of the EGP and the Kalgoorlie

Terrane developed predominantly through province-wide ~E-W shortening. Swager and

Nelson (1997) recognized four main compressive deformation episodes (D1-D4, Table

2.1) in the Kalgoorlie Terrane, each preceded by extensional periods (De). The volcano-

sedimentary sequence was deposited during De - the earliest extensional phase. South

over north compression (D1) followed at > 2675 Ma and led to thrust faulting and

widespread structural repetition (Swager and Nelson, 1997). Coarse clastic sequences

were deposited during a second extensional phase that preceded regional D2 shortening.

Widespread granitoid intrusion also accompanied this extensional phase (Weinberg et

al., 2003). Approximately E-W shortening during regional D2 (2675-2657 Ma, Nelson,

1997) resulted in NNW-SSE trending upright folds and penetrative foliation (Swager,

1989; Swager and Griffin, 1990; Weinberg et al., 2003). Deformation during D3 (2663-

2632) and D4 (<2640) (Nelson, 1997; Swager, 1997) changed from oblique-slip to

strike-slip in nature and progressed from a ductile to a brittle regime (Mueller et al.,

1988; Bateman et al., 2001). Recent studies have proposed a more complex

deformational history for the Kalgoorlie Terrane than that encompassed by the widely

accepted D1-D4 nomenclature. Blewett et al. (2004) proposed that D2 deformation was

episodic, involving switching between extensional and compressional tectonic regimes,

and that it was diachronous across the EGP. Weinberg et al. (2005) do not consider D3

and D4 to be separate tectonic events, as they are not separated by a significant time gap

and formed with the same strain orientation. They consider that these two events reflect

different expressions of the same tectonic event as the crust cooled or strain rate

increased.

2.3 The Boulder-Lefroy Fault Zone

The Boulder-Lefroy fault zone (BLFZ) is an interpreted first-order crustal-scale

fault system (e.g., Swager, 1989) located on the eastern margin of the Kalgoorlie

Terrane (Fig. 2.1) in the Eastern Goldfields Province of the Yilgarn Craton. The fault

extends over 200 kilometers in length from north of Kalgoorlie to south of Kambalda

(Gemuts and Theron, 1975; Griffin, 1990). At New Celebration, the BLFZ truncates the

eastern limb of the Celebration Anticline (Archibald, 1992) (Fig. 2.2) and has a

complicated history with a number of different interpretations regarding its movement

sense. Most researchers (e.g. Swager, 1989) concur that the major period of fault


26

Table 2.1 Summary of deformation events in the Eastern Goldfields Province. Modified

from Blewett et al. (2004). Events Structures Granites References

?De Low angle shear on granite-greenstone contacts; N-S movement; polydirectional extension, local recumbent folding

High-Ca Hammond and Nisbet (1992), Passchier (1994)

D1 D1c

Low-angle thrust faults and recumbent folds; shear on early granitoid greenstones contacts; late synvolcanic slides caused by uplift?

Archibald et al. (1978), Swager and Griffin (1990), Swager (1997)

D1e Deformed contacts between early granitoid complexes and greenstones; N-S lineations in contact zone; recumbent folds in overlying greenstones

Witt (1994)

D2 E-W compression developing upright folds with shallowly NNW to N-plunging fold axes, axial planar foliation and crenulation.

High-Ca Hammond and Nisbet (1992), Krapez. et al. (2000), Weinberg et al. (2003)

D3 Tightening of F2 folds; NW to NNW sinistral strike-slip faults and shear zones; N to NNE dextral strike-slip faults and shear zones. Transpression on NNW faults, with compressional jogs and fold axes trending N to NNE

Swager (1997), Witt (1994), Chen et al. (2001)

Late D3

Steeply plunging lineations on strike-slip faults. Steeply dipping reverse faults

Low-Ca/syenite

Witt (1994); Smithies and Champion (1999)

Late D3e

Post-metamorphic orogenic collapse Swager (1997)

D4 NW to WNW oblique sinistral faults; NE to ENE oblique dextral/reverse faults

Archibald et al. (1978), Witt (1994)

formation and movement occurred during D3, however, the movement sense and

interpretation of the fault system varies. Swager (1989) described the BLFZ as a major

oblique, sinistral wrench structure, active during D3, with an apparent sinistral

displacement of 12 kilometers, indicated by segmentation of the Stony Hill-Mt Goddard

Dolerite into strike-slip duplexes and asymmetrical relationships with regional fold

structures. Various authors proposed reverse movement along the BLFZ, based on

seismic data (Goleby et al., 2000) and field observations (Boulter et al., 1987; Copeland,

1998; Ridley and Mengler, 2000). Others have proposed oblique-sinistral movement

(Swager, 1989; Witt, 1991; Nguyen et al., 1998; Nichols, 2003) and dextral movement.

Mueller et al. (1988) described two stages of wrench faulting on the BLFZ; an early

phase of sinistral transpressional shearing during D2 followed by a later phase of dextral

transcurrent shearing, with a thrust component, during D3. Weinberg et al. (2005)

described a two-stage process for the formation of the BLFZ, in which isolated north-

south trending thrust ramps, formed during D2 ~east-west compression, coalesced into a

single cohesive fault zone during D3 sinistral strike-slip reactivation. Nichols (2003)

described D3 sinistral oblique-slip and post-D3 horizontal strike-slip movement of

unknown direction at New Celebration.


27

Figure 2.2 Geological map of the New Celebration district illustrating the Celebration

anticline and major deposits (redrawn from Swager, 1989).

APPENDICES 28

28

There are a number of factors contributing to discrepancies between authors

when describing the kinematic history of the BLFZ. The fault has a strike length of over

200km although along most of its length the fault trace is poorly exposed, and is

complicated by a number of different splays (Griffin, 1990). Further, some authors (e.g.

Swager, 1989) consider the Boulder fault to the north, and the Lefroy fault to the south,

as separate entities. Outcrops are sparse and there are few locations where structural

measurements and observations can be taken directly from within the fault.

Additionally, the fault has had a long-lived and complex deformation history and has

been active in various forms throughout orogenesis.

2.4 Distribution and Timing of Gold Mineralization

The Yilgarn craton has produced over 2,500 tonnes of gold from over 10,000

deposits in the last 120 years (Townsend et al., 2000). A significant number of those

deposits occur in the Kalgoorlie Terrane and the largest are associated with the BLFZ.

The BLFZ hosts the New Celebration gold deposits (2 million ounces) and is spatially

correlated with the Golden Mile deposit, which at >50 million ounces contained gold

(Bateman and Hagemann, 2004) is the largest orogenic lode gold deposit in the world,

and St Ives (>8 million ounces production, pers. comm. Justin Osborne, 2007). Both

these deposits occur within second- and third-order structures adjacent to the main trace

of the BLFZ. Weinberg et al. (2005) noted that the major gold mining districts along the

BLFZ were distributed 30 to 40 kilometers apart, and that the more gold-endowed

districts were flanked by the least endowed districts adjacent along strike. Further, the

largest gold deposits (Golden Mile, New Celebration, St Ives) coincide with the

exposure of regionally significant anticlinal cores.

The timing of gold mineralization in the Yilgarn craton is contentious.

Traditional models consider that gold mineralization within Archean terranes occurred

late in the evolution of the host terrane (Colvine et al., 1988; Groves et al., 1989;

Kerrich and Cassidy, 1994) during the final stages of volcanism and coincident with

spikes in plutonism and deformation (Robert et al., 2005). Within the regional structural

framework of Swager (1989), published age determinations constrain gold

mineralization in the Yilgarn craton to the period 2660 to 2625 Ma (Groves et al., 2000;

Mueller, 2007), over a restricted time interval during late D3, post-peak metamorphism

and associated with reactivation of crustal-scale deformation zones (Groves, 1993). A

number of different deposits in the Kalgoorlie terrane associated with the BLFZ, such as

APPENDICES 29

29

Victory, (Clark et al., 1986); Revenge (Nguyen, 1997) and New Celebration Stage I

(Nichols, 2003) appear consistent with this hypothesis. The Golden Mile, however,

which is the largest gold deposit in the EGP, and at least one stage of mineralization at

New Celebration, appear to contradict this model.

In Kalgoorlie, Groves (1993) considered the Fimiston lodes at the Golden Mile

to be syn-D3 (2660 to 2632 Ma, Nelson, 1997; Swager et al., 1997). Recent work on the

Golden Mile deposit however, based on structural relationships and dating of

intermineral dikes, indicates that the Fimiston and Oroya lodes may be much older,

possibly late D1 to early D2 (Bateman et al., 2001; Bateman and Hagemann, 2004;

Gauthier et al., in revision). Further, structural evidence indicates that the Mt Charlotte

lodes at the Golden Mile formed during D4 brittle-ductile faulting. Bateman et al.

(2001) and Bateman and Hagemann (2004) interpreted all of these data as indicating

that gold mineralization in the Kalgoorlie camp was a protracted event, which occurred

over a period of approximately 50 Ma and which formed different deposit styles.

Nichols (2003) also identified a late-stage mineralization event at New Celebration

associated with brittle-ductile deformation and interpreted, based on cross-cutting

relationships, those as post-D3 (likely D4) but otherwise unconstrained.

CHAPTER THREE: GEOLOGY OF THE NEW CELEBRATION GOLD DEPOSIT

30

3 CHAPTER THREE: GEOLOGY OF THE NEW CELEBRATION GOLD DEPOSIT

3.1 Mine Stratigraphy

The New Celebration gold deposit is hosted within a sequence of folded and

sheared komatiites, differentiated dolerites and felsic volcaniclastic rocks, which have

been intruded by several generations of felsic and lamprophyric dikes and truncated by

the BLFZ. Langsford (1989) established the stratigraphy of the New Celebration deposit

and correlated it to the stratigraphic sequence established for the Kalgoorlie-Kambalda

corridor by Gresham and Loftus-Hills (1981), Swager (1989), Swager et al. (1995) and

Watchorn (1998) (Table 3.1). The 200-metre thick Kambalda Komatiite comprises the

basal stratigraphic unit (Fig. 3.1) at New Celebration and forms the footwall in the

Hampton-Boulder and Jubilee open pits. Typically, this unit is fine-grained,

equigranular and homogeneous (Watchorn, 1998) and serpentine, tremolite, chlorite and

talc replace primary mineralogy. Low-strain zones preserve relict primary spinifex and

cumulate textures pseudomorphed by magnetite and talc (Copeland, 1998). The upper

contact of the Kambalda Komatiite is conformable with the overlying differentiated

dolerite and is intensely sheared and hydrothermally altered in the BLFZ.

The hanging wall at the New Celebration deposit is a differentiated mafic unit,

locally termed the Jubilee Dolerite but stratigraphically equivalent to the regional

Pernatty Dolerite (Langsford, 1989; Norris, 1990; Archibald, 1992; Copeland, 1998).

Six main zones comprise the Pernatty Dolerite: (1) a 50-200m thick basal cumulate

pyroxenite; which grades into (2) a melanocratic dolerite characterized by coarse-

grained (up to 20 mm long) pyroxene phenocrysts in a fine-grained plagioclase

groundmass; (3) equigranular magnetite-rich dolerite; (4) equigranular magnetite-rich

granophyre; (5) fine-grained oxide-rich dolerite with characteristic bladed pyroxene

phenocrysts; and (6) a fine-grained chill zone (Archibald, 1992). The mafic rocks show

metamorphic mineral assemblages typical of greenschist facies metamorphism (1994),

however, the original igneous textures are preserved (cf. Gresham and Loftus-Hills,

1981).

Nichols (2003) recognized two major magmatic events at New Celebration,

based on mineralogy, deformation style and cross-cutting relationships. Early intensely

carbonate-biotite-magnetite altered plagioclase porphyry dikes are


31

Table 3.1 Stratigraphy of the New Celebration deposits correlated with the regional frameworks

established for Kalgoorlie and Kambalda

Kalgoorlie (Swager, 1989, Swager et al. 1995) New Celebration (Langsford, 1989) St Ives (Watchorn, 1998)

Kurrawang Formation: Alluvial, fluviatile and shallow-marine coarse clastic sandstone deposited within locally fault-bounded synclines parallel to regional tectonic trend

Merougil Conglomerate Merougil Conglomerate

Black Flag Group: Felsic volcanic and volcaniclastic sedimentary sequence, >1km thick, coarsening upwards

Black Flag Group Black Flag Group

Golden Mile Dolerite: Differentiated tholeiitic dolerite, divided into 10 petrographic units, 800m thick

Triumph Gabbro Condensor and Junction Dolerites

Kalgoorlie Group Paringa Basalt: Up to 1500m thick, high Mg, variolitic, pillowed, cherty interflow sediments

Kyarra Basalt Paringa Basalt

Williamstown Dolerite: Up to 300m thick, fractionated

Pernatty Dolerite, 300-500m thick, basal cumulate pyroxenite

Defiance Dolerite

Kapai Slate: Marker horizon, 5-25m thick, pyritic graphitic slate to magnetite-bearing chert

Kapai Slate Kapai Slate

Devon Consols Basalt: 60-100m thick, high Mg variolitic basalt

Mutooroo Basalt, 100-200m thick Devon Consols Basalt

Hannan's Lake Serpentinite: 800-1200m thick, serpentinized ultramafic lavas grading upward to high Mg basalt

Kambalda Komatiite Kambalda Komatiite

Lunnon Basalt: >200m thick, pillowed tholeiites with thin interflow sediments

denoted M1 and have a penetrative foliation. These intrusions are crosscut by weakly

albite-carbonate-magnetite-hematite altered, nonfoliated to weakly foliated quartz-

feldspar porphyry dikes, designated M2, which preserve primary igneous textures. The

M2 porphyries are up to 80m thick, extend over 400m along strike and down dip

(Copeland, 1998) and are boudinaged along strike and down dip. Other intrusive phases

such as quartz-phyric felsic porphyry dikes, lamprophyres (Nichols, 2003) and shear-

parallel intermediate porphyries (Williams, 1994) are associated with gold

mineralization but are volumetrically insignificant. The mine sequence, with the

exception of the M2 porphyries, is metamorphosed to upper greenschist facies (Norris,

1990).


32

Figure 3.1 Lithostratigraphy of the New Celebration deposit, modified from Nichols (2003)

3.2 Mine Deformation Events and Regional Correlation

Nichols (2003) identified three main deformation events at New Celebration,

and tentatively correlated them with regional deformation events (Table 3.2). For clarity

Nichols (2003) marked or denoted the local New Celebration events with the subscript

NC; this convention is maintained throughout the thesis. An event correlating to

regional D1 was not recognized at the New Celebration gold deposits. Vertically tilted

conformable stratigraphic contacts characterize D2NC, the earliest recognized

deformation event at New Celebration. This event corresponds to the regional D2

upright folding of Swager (2003) and Swager and Griffin (1989). Steeply southwest-

and west-southwest-dipping, northwest- trending S-C fabrics, south-southwest-plunging

mineral elongation lineations and sigmoidal quartz grains constrain movement on the

BLFZ during D3NC as sinistral oblique slip, west-block-down to the southwest (Nichols,


33

2003). This tentatively correlates with regional D3 ENE-WSW compression and

sinistral strike- and dip-slip faulting (Nichols, 2003; Nichols et al., 2004). Northwest-

dipping structures and a second penetrative northeast-trending, northwest-dipping S-C

fabric, which crosscut S3NC, represent D4NC and constrain fault movement during D4NC

as sinistral strike slip. Quartz-carbonate-chlorite-epidote veins that crosscut D3NC

foliation are also assigned to D4NC. Late curviplanar faults that crosscut all other

structures are assigned to D4+NC. In contrast, Weinberg et al. (2005) identified two

phases of movement at New Celebration (Table 3.2), an early phase of movement

characterized by crustal shortening and vertical extension during D2 and a later

movement phase characterized by clockwise rotation of the maximum shortening axis

from east-northeast–west-southwest to east-southeast–west-northwest and reactivation

of north-northwest–trending thrust planes by sinistral shear zones, during D3.

3.3 Gold Mineralization and Hydrothermal Alteration

The New Celebration gold deposit comprises six open pits (Hampton-Boulder,

Jubilee, Mutooroo, Celebration, Golden Hope, and Early Bird) and the Hampton

Decline underground operation, which comprises four ore zones (Southern, Central,

Northern, and B40). Collectively the deposits produced approximately 1.5 million

ounces of gold between 1987 and 1997, with the majority of the gold exploited in open

pits from the Hampton-Boulder (7.4Mt @ 2.34 g/t Au for 560,000 oz (Dielemans,

2000)) and Jubilee (10.3Mt @ 2.09 g/t Au for 693,000 oz) deposits. These two deposits,

which since December 2007 have comprised a single resource under the ownership of

Dioro Exploration NL, are the focus of this study.

Mafic schists, mylonites and sheared intermediate porphyritic intrusions and

felsic porphyries host gold mineralization within brittle-ductile shear zones and brittle

quartz breccias (Swager, 1989; Swager and Griffin, 1990). Ore zones are located in the

hanging wall of a steeply dipping, deformed contact between mafic and ultramafic

rocks, and are spatially associated with, and hosted within, intermediate and quartz-

feldspar porphyry dikes that intruded the contact along the BLFZ (Williams, 1994;

Nichols, 2003) (Figs. 3.2, 3.3). Nichols (2003) identified two mineralizing events, Stage

I and Stage II, and four mineralization styles (Mylonite, Porphyry, Contact and

Fracture) classified according to the host rocks and their mode of occurrence . Stage I

gold mineralization is associated with ductile deformation and is hosted within fine-

grained deformed pyrite along foliation planes in mylonitized and deformed

intermediate M1 porphyry and mafic schists. Stage II gold mineralization is associated


34

.

Figure 3.2 Interpreted geology of the New Celebration open pit showing the location of the BLFZ within

the pit, the location of the ore zones, diamond drill holes logged and sampled in this study and in Nichols

(2003), and strike and dip of S3NC foliations. A-A' is section shown in Fig. 3.3. Modified from Nichols

(2003).

A

A'


35

Table 3.2 Deformation of the New Celebration deposits correlated with regional deformation events and the deformation sequences established for Kalgoorlie and Kambalda

Age Regional Deformation Kalgoorlie Gold Camp (Bateman and Hagemann, 2004)

New Celebration Gold Camp (Nichols, 2003)

Kambalda Gold Camp (Archibald, 1985; Swager, 1989; Nguyen, 1997)

<2640 (Swager, 1997)

D4 dextral shear on NNE-SSW trending shear zones

D4 Right lateral oblique-slip movement on NNE striking faults

D4NC Strike slip movement on the BLFZ. Movement sense unconstrained

D4 NE-SW shortening. Reactivation of pre-existing faults and development of brittle NE and NW faults

2663-2645 (Nelson, 1997; Swager, 1997)

D3 Strike-slip shear with dextral and sinistral movement

D3 Broad scale left lateral transpression resulting in sinistral strike-slip movement on the BLFZ and BS and local scale antithetic right lateral strike slip movement on NNE striking, steeply NW dipping faults

D3NC Sinistral oblique-slip west block down to the SW movement on the BLFZ

D3 ESE-WNW shortening. Sinistral movement on N-trending faults, tightening of D2 folds, reactivation of D2 faults and development of new faults subsidiary to D2 faults

2675-2657 (Nelson, 1997)

D2 ENE-WSW regional shortening, upright foliation and folds (Swager, 1997; Witt and Swager, 1989; Nelson, 1997; Ridley and Mengler, 2000)

D2 NE-SW compression. Development of NNW striking thrust faults, upright folds and NS striking, subvertical axial planar cleavage

D2NC Tilting of conformable sub-units of the Pernatty dolerite to vertical orientations

D2 ENE-WSW shortening,. Development of open upright folds such as the Kambalda Dome, and development of main upright (S2) foliation

>2675 (Swager 1997)

D1 Low angle shears, thrusting, stratigraphic repetition, recumbent folds (Swager, 1989; Passchier, 1994, 1995; Swager and Nelson 1997)

D1 (local)

NE-SW compression. Development of N-trending, NE over SW thrust faults and Kalgoorlie Anticline

D1 N-S compression. Development of E-W-trending thrust faults and recumbent folds such as the Foster, Tramways and Republican thrusts.


36

Figure 3.3 East-West cross section of the southern portion of the Hampton Boulder Jubilee deposit. The

M1plagioclase-rich porphyries form thin, ribbon-like bodies confined to the ultramafic footwall, whereas

boudinaged M2 quartz-feldspar porphyry has intruded throughout the mafic-ultramafic contact, hanging

wall and footwall. Modified from Nichols (2003). tl-cl-cb=talc-chlorite-carbonate.

with brittle- ductile deformation and is hosted within high magnesium basalt and felsic

porphyry dikes. These dikes crosscut and intrude the Stage I-hosting M1 porphyries,

which indicate that the mineralization stages are separated in time, although their

absolute ages are presently unconstrained

3.3.1 Pre-gold and Regional Alteration

Widespread carbonate (dominantly calcite) alteration, unrelated to gold mineralization,

is ubiquitous throughout the New Celebration mine sequence (Langsford, 1989; Norris,

1990) and likely represents alteration from regional scale, fault controlled mantle-

derived carbonaceous fluids (cf. Barley and Groves, 1987) associated with D2-D3

deformation in the Kalgoorlie Terrane along the BLFZ. Regional metamorphic talc-

carbonate alteration characterizes the footwall ultramafic rocks, whereas the hanging

wall mafic units are chlorite-carbonate altered (Norris, 1990). Fine-grained, anhedral

magnetite is extensive and ubiquitous throughout the hanging wall mafic schists,

intermediate porphyries and the footwall ultramafic unit (Williams, 1994). Its

A A'


37

widespread distribution and abundance throughout the deposit, both proximal and distal

to mineralization and its equilibrium textural relationship with syn-S3NC biotite

(Williams, 1994; Weinberg et al., 2005) indicates that magnetite likely formed during

regional D3 metamorphism, with Fe derived from the metamorphic devolatilization of

the underlying mafic stratigraphy. Fine-grained subhedral magnetite and ilmenite

overprint the primary igneous fabric in high-Mg basalt.

3.3.2 Stage I Gold Mineralization and Related Alteration

Stage I gold occurs as rounded inclusions within disseminated, deformed fine-grained

pyrite, which is aligned parallel to the S3NC foliation planes (Fig. 3.4) in mafic schists

and strongly foliated to mylonitic M1 porphyry, or within syn-D3NC quartz-calcite-

pyrite veins. Ankerite and hydrothermal quartz pressure shadows developed on the

margins of the host pyrite within the foliation planes indicate that pyrite and gold

precipitation was concomitant with D3NC deformation. Biotite-ankerite-albite-sericite-

pyrite alteration and a strong telluride association characterize Stage I gold

mineralization. Alteration zones are poorly defined for Stage I mineralization as the M1

porphyries in particular are pervasively hydrothermally altered (Nichols, 2003). The

intensity of proximal bio-ank-alb-ser-py alteration increases with proximity to, and

abundance of quartz-carbonate veins, however, as does gold grade. Pyrite replaces pre-

existing magnetite alteration and, in addition to gold inclusions, some grains contain

trace magnetite, hematite, galena, chalcopyrite and pyrrhotite inclusions. Stage I

represents the highest grade gold mineralization at New Celebration and is the

significant gold event in terms of tonnage and grade (>3 g/t Au) (Copeland, 1998).

3.3.3 Stage II Gold Mineralization and Related Alteration

Stage II gold is observed as intragranular inclusions or along grain boundaries within

pyrite at the contact between high-Mg basalt and M2 quartz-feldspar porphyry and in

pyrite within quartz-sericite-pyrite veins developed on the margins of the felsic

porphyry dikes (Fig. 3.5). In contrast to Stage I, Stage II gold-hosting pyrite is coarse-

grained, predominantly euhedral, and where it occurs at the mafic-felsic contact,

overprints the S3NC foliation wrapping the felsic porphyry dike (Fig. 3.5). The proximal

alteration assemblage comprises ankerite-sericite-quartz±chlorite and is zoned around

the contact. It extends approximately 40 cm from the mafic-felsic contact.


38

Figure 3.4 Photographs and photomicrographs of representative Stage I gold mineralization samples

illustrating proximal gold-related alteration and gold location. A. Quartz-ankerite and biotite-sericite

alteration defining S3NC foliation with syn-S3NC gold-hosting pyrite from Mylonite-style mineralization.

B. Biotite defining S3NC foliation in M1 porphyry. C. Pyrite in textural equilibrium with S3NC foliation,

defined by biotite, in Porphyry-style mineralization. D. Back-scattered electron image of a rounded gold

bleb within syn-S3NC pyrite from Mylonite-style mineralization. A, B and D from Nichols (2003).

Bt=biotite, Ab=albite, Ser=sericite, Ank=ankerite, Py=pyrite, Qz=quartz.

Pyrite abundance and gold concentration increases with proximity to the mafic-felsic

contact. Tellurides were not observed in Stage II gold mineralization. The location of

Stage II gold mineralization within undeformed M2 porphyries, which crosscut Stage I

gold-hosting M1 porphyries, and the occurrence of gold in euhedral pyrite that

overprints the S3NC foliation, indicate that Stage II post-dates Stage I and is interpreted,

therefore, to post date D3NC. Gold grade in Stage II is inversely proportional to the

width of the M2 porphyry, i.e. the highest grades are developed where the porphyry is at

its narrowest, and where the density of type 3 quartz-pyrite and type 4 sericite-pyrite


39

Figure 3.5 Photographs and photomicrographs of representative Stage II gold mineralization samples

illustrating proximal gold-related alteration and gold location. A. Contact-style mineralization. Ore-

hosting pyrite at contact between ankerite-sericite altered high-Mg basalt and ankerite-sericite altered

albitized M2 porphyry. B. Coarse-grained euhedral ore-stage pyrite overprinting S3NC foliation. C.

Sericite-pyrite veins in M2 porphyry. D. Coarse-grained gold along pyrite grain boundaries in Fracture-

style mineralization

veins is highest. Stage II gold mineralization is characterized by lower gold grades

(<3g/t Au) and lower tonnage when compared to Stage I gold mineralization (Norris,

1990; Copeland, 1998).

3.3.4 Post Gold Alteration

Nichols (2003) recognized a number of post-gold alteration events at New

Celebration. Coarse-grained hornblende veins cross cut D3NC foliation and Stage I gold-

related pyrite. Randomly oriented, coarse-grained euhedral actinolite-tremolite spatially

associated with M2 felsic dikes overprints deformation fabrics in ultramafic footwall


40

rocks. Late-stage coarse-grained euhedral carbonate overprints the actinolite-tremolite

and is in turn overprinted by fine-grained euhedral magnetite. Williams (1994)

described ubiquitous, heterogeneously distributed hematite staining throughout the

southern ore zone. He noted that flat-lying quartz-carbonate-chlorite veins (also

observed by Nichols, 2003), which crosscut mineralized veins and associated alteration,

controlled the distribution of hematite alteration. Figure 3.6 summarizes the

deformation, mineralization and alteration paragenesis of New Celebration


41

De Emplacent of volcano-sedimentary sequence

D1 No recorded event at New Celebration

D2NC East-west oriented compression Tilting of stratigraphic contacts to vertical Formation of proto-BLFZ

Early D3NC Development of BLFZ as mantle tapping structure Emplacement of M1 porphyry Widespread mantle C alteration Type 1 Qz-cc boudinaged veins

Mid D3NC Peak metamorphism Magnetite alteration

Mid-Late D3NC Type 2 qz-cc-py veins Stage I Au bi-ank-ser-ab-py alteration Au, py, cpy, gn, po

Late D3NC Hornblende veins overprinting Au mineralization

Late D3NC-Early D4NC Emplacement of M2 porphyry Type 3 qz±cb, ser, py veins Type 4 ser-py veins Stage II Au ank-ser-qz-chl-py alteration Au, py

Post D4NC Actinolite-tremolite alteration Carbonate overprint Late magnetite


42

Figure 3.6 (Previous Page) Deformation, alteration and mineralization paragenesis of the New

Celebration gold deposit

3.4 Vein Paragenesis and Petrography

3.4.1 Vein Types

Four major vein groups that correlate with specific deformation events and gold

mineralization styles were identified at New Celebration (Fig. 3.7, Table 3.3). Type 1

quartz-calcite boudinaged veins formed prior to D3NC and predate gold mineralization.

Type 2 quartz, calcite and quartz-calcite veins developed during D3NC and were

synchronous with Stage I gold mineralization. Type 3 quartz breccia veins developed

during late D3NC or post D3NC and crosscut Stage I gold mineralization. Type 4 sericite-

pyrite veins formed during D4NC and host Stage II gold mineralization.

3.4.2 Vein Mineralogy and Textures

Type 1 veins are foliation-parallel quartz-calcite veins, which occur in mylonites

and strongly foliated M1 plagioclase porphyries (Fig. 3.7a). Quartz and calcite grains

exhibit undulose extinction and have undergone complete dynamic recrystallization by

grain boundary migration and sub-grain rotation.

Type 2 veins comprise predominantly quartz and calcite with accessory pyrite

and ankerite. They may be parallel or perpendicular to S3NC foliation and are interpreted

to have formed synchronous with D3NC deformation, and therefore Stage I

mineralization, based on mutually cross-cutting relationships with the foliation planes in

veins that formed perpendicular to S3NC foliation (Fig. 3.7b). Vein density and

abundance increases with gold grade, as does pyrite abundance, with up to 10%

disseminated pyrite and 5-7% type 2 veins observed in higher grade zones. Type 2 veins

are typically surrounded by wide (20-50 mm) ankerite alteration zones and clusters of

large, inclusion-rich pyrite grains along the vein selvedges. These pyrite grains typically

exhibit a “dirty”, inclusion-rich core surrounded by a “clean”, inclusion-free rim.

Inclusions comprise abundant silicates, minor sulfides (galena, sphalerite), iron oxides

(magnetite, hematite, ilmenite) and rare gold blebs. Quartz grains in type 2 veins have

undergone partial dynamic recrystallization by grain boundary migration and sub-grain

rotation. Grain boundaries are commonly highly irregular and protrude into neighboring

grains, although the degree to which individual samples have been recrystallized varies.

Sub-grain development is minor and is predominantly concentrated along the outer vein


43

Figure 3.7 Photographs of dominant vein types. A. Type 1 foliation-parallel quartz±calcite veins. B. Type

2 zoned quartz-calcite veins showing mutually cross-cutting relationship with S3NC foliation. C. Type 3

coarse-grained quartz veins cross-cutting contact between M2 quartz-feldspar porphyry and high Mg

basalt. D. Thin Type 4 sericite-pyrite veins in M2 quartz-feldspar porphyry.

Table 3.3 Summary of main vein type characteristics, deformation, structure and timing.

Vein Type

Deformation Event Timing Mineralogy Width

(mm) Mineralization Structure Alteration Halo

1 D2NC Syn-D2NC Quartz, carbonate 2-10 Deformed, boudinaged recrystallized veins parallel to D3NC foliation

Ankerite?

2 D3NC Syn-D3NC Quartz, calcite, pyrite

2-30 Py, Cpy, Sl, Gn, Au, Tell

Thin veins, show mutually cross-cutting relationships with D3NC foliation

Ankerite

3 D3NC or D4NC Late D3NC or D4NC. Cross-cut D3NC foliation

Quartz, (carbonate, sericite, pyrite)

5-50 Py, Form brittle vein arrays

None

4 D3NC or D4NC Late D3NC or D4NC. Cross-cut D3NC foliation

Sericite, pyrite 1-3 Py, Au Thin veinlets None


44

edge. Relict grains locally exhibit undulose extinction and lattice-preferred orientation

(cf. Passchier and Trouw, 1996).

Type 3 veins comprise quartz, calcite and sericite with minor coarse-grained

subhedral to euhedral pyrite. The veins are composed almost entirely of coarse-grained

(1-5 mm) clear quartz overprinted by accessory calcite and rare sericite. The veins

brecciate the host M2 quartz-feldspar porphyries and crosscut S3NC foliation (Fig. 3.7c).

They can be distinguished from type 2 veins by their coarse grain size, minor amount of

calcite and lack of an alteration selvedge. Locally, some quartz grains within these veins

have diffuse and highly irregular grain boundaries indicating partial dynamic

recrystallization by grain boundary migration.

Type 4 veins, which host Fracture-style mineralization, are composed of sericite,

chlorite and pyrite, and form thin (1-2 mm) stringer veins (Fig. 3.7d). These veins are

only located in M2 quartz-feldspar porphyries. Where type 4 veins crosscut earlier

quartz breccia veins, they have generally developed along the quartz grain boundaries.

Pyrite occurs as large (up to 2 mm) subhedral to euhedral grains or as aggregates of fine

subhedral to euhedral crystals, and commonly contains abundant silicate and sulfide

inclusions. Pyrite hosts gold as rounded inclusions within grains and localized along

pyrite grain boundaries

3.5 Summary

Host rocks, vein and sulfide mineralogy and cross cutting relationships separate

gold mineralization at New Celebration into two distinct events: Stage I associated with

ductile strike-slip deformation at the BLFZ, after peak metamorphism, and Stage II

associated with brittle-ductile reactivation of the BLFZ.

Stage I gold mineralization took place after regional peak metamorphism during

D3NC deformation (Witt, 1993a; Copeland, 1998; Nichols, 2003) and formed within

ductile, oblique-slip, shear zones, hosted within magnetite-altered intermediate

composition plagioclase (M1) porphyry and mylonitized mafic schists. Gold

mineralization is associated with type 2 syn-deformational quartz-calcite-pyrite veins

and proximal biotite-albite-ankerite-sericite-pyrite alteration. Gold typically formed as

rounded blebs within deformed pyrite in textural equilibrium with D3NC foliation planes

and is commonly associated with both Au- and non Au-bearing tellurides. Vein

abundance and density and pyrite abundance increases with increasing gold grade


45

within the ore zones, and the development of proximal alteration assemblages appears

to be directly correlated to the presence and abundance of type 2 veins.

The development of metamorphic magnetite in M1 porphyries and mafic schists

appears to be a significant factor in the development of gold mineralization in these

otherwise Fe-poor rocks during Stage I. The strong positive correlation between

increasing gold grade and modal pyrite abundance, and the replacement of metamorphic

magnetite with pyrite in M1 porphyries and mafic schists indicate that gold precipitated

by sulfidation of wall rock iron oxides. The development of metamorphic magnetite

enriched the host rock in iron, which facilitated the sulfidation process (cf. Phillips,

1986) and led to the development of Stage I gold mineralization

Stage II mineralization formed during brittle reactivation of the BLFZ during

late D3NC and early D4NC (Nichols, 2003). Gold mineralization is associated with the

emplacement of M2 quartz-Kspar phyric felsic porphyry into the BLFZ, which took

place after the onset of peak metamorphism, as evidenced by the lack of D3NC foliation

within the porphyry and the absence of metamorphic minerals (Nichols, 2003). Gold

formed at the contact between M2 porphyry and high-Mg basalt, and associated with

type 3 quartz and type 4 sericite-pyrite veins within the porphyry. Replacement of wall

rock oxides by pyrite in high-Mg basalt along the contacts of the porphyry indicate that

sulfidation reactions were a significant component in forming Stage II gold, at least for

Contact style mineralization.

Table 3.4 Summary and comparison of characteristics of Stage I and Stage II gold mineralization at New Celebration

Event Timing Structural Regime

Host Rocks Veins Grain Size

Alteration assemblage

Associated sulfides

Stage I D3NC Ductile M1 porphyry and mafic schist

type 2 qz-cc-py

1-2 µm

bio-ank-alb-ser-py

gn, cpy, po, sl

Stage II Late D3NC-D4NC

Brittle-ductile

M2 porphyry and high-Mg basalt-porphyry contact

type 3 qz and type 4 ser-py

250 µm

ank-ser-qz±cl

gn, cpy, sl

CHAPTER FOUR: INTEGRATED FLUID STUDY

46

4 CHAPTER FOUR: INTEGRATED FLUID STUDY Archean orogenic lode-gold deposits worldwide typically show a close spatial

relationship with first-order, crustal-scale shear zones (Eisenlohr et al., 1989; Neumayr

et al., 2000), however, at camp- to deposit- scales, , second- and third-order splays host

the majority of world class (>100t Au) orogenic lode gold deposits (Eisenlohr et al.,

1989; Groves, 1990). There has been very little research undertaken on the P-T-X-t

evolution of hydrothermal fluids in first order system, predominantly because they

mostly do not directly host gold mineralization , but is also due to the poor exposure of

first order fault systems. Given its location within the BLFZ, an interpreted first-order

crustal-scale fault zone spatially correlated with one giant and two world-class gold

camps, New Celebration provides a unique opportunity to study the P-T-X-t-d evolution

of hydrothermal fluids in a crustal-scale fault zone and evaluate the role regional

structures play in focusing mineralizing and non-mineralizing fluids.

The integrated fluid study of the New Celebration deposit was undertaken to: (1)

document the fluid evolution in pressure-temperature-composition (P-T-X) space of the

western segment of the Boulder Lefroy Fault Zone at the New Celebration gold deposit;

(2) establish a paleohydrothermal fluid model for the New Celebration gold deposit; (3)

characterize the metal content of mineralizing and non-mineralizing fluids at the New

Celebration gold deposit; and (4) evaluate potential fluid source(s) for both the

mineralizing and non-mineralizing fluids;.

4.1 Sample Selection, Preparation and Analytical Procedures

4.1.1 Sample Selection and Preparation

Seven diamond drill holes within the Hampton-Boulder and Jubilee open pits

and underground workings were logged and sampled for this study. The chosen holes

were selected because they intersected the hanging wall, ore zones and footwall at

depths from the present surface to 250 m below the pit floor, they all contained high-

grade (>3.0 g/t Au) ore zones and more than one mineralization style was represented in

each hole. Approximately 70 samples representing the different mineralization styles

and stages were collected for further analysis. Of these, 18 quartz and calcite vein

samples were prepared as 80 µm double-polished thick sections and then

petrographically examined for quartz textures and fluid inclusions. Six samples

representing type 1 (one), type 2 (two), type 3 (two) and quartz-carbonate alteration


47

associated with Contact-style mineralization (one) contained fluid inclusions large

enough (>5 µm) to conduct detailed microthermometric and laser Raman analyses.

The samples were examined petrographically prior to microthermometric

analysis in order to categorize the morphology, distribution and relative timing of fluid

inclusions with respect to the host quartz and carbonate crystals. These petrographic

observations in conjunction with low-temperature microthermometry and laser Raman

analyses were used to determine the fluid inclusion types and to identify fluid inclusion

assemblages (Goldstein and Reynolds, 1994). Over 500 microthermometric

measurements on fluid inclusions were collected in quartz from type 2 quartz-calcite

veins, type 3 quartz veins, and from quartz alteration associated with Stage II gold

mineralization. Type 1 boudinaged veins contained only rare inclusions suitable for

analysis due to the almost complete dynamic recrystallization of the quartz. Suitable

inclusions in calcite (type 2 quartz-calcite veins) did not appear to have undergone any

post-entrapment modifications; therefore, they were also measured. Fluid inclusions in

all samples typically ranged in size from <1 µm to approximately 30 µm and varied in

morphology from highly irregular to rounded to negative crystal shaped.

4.1.2 Microthermometry Procedures

Microthermometric data were collected using a fully automated Linkham

THMSG heating and freezing stage, which has a temperature range of -196 °C to +600

°C. The stage was calibrated against the melting point of pure CO2 (-56.6 °C) and pure

H2O (0.0 °C), and the critical point of pure H2O (374.1 °C) using SynFlinc synthetic

fluid inclusion standards. Accuracy of the stage during low-temperature (<32 °C)

measurements was between ± 0.1 °C and ±0.4 °C and during high temperature

measurements (>100 °C) was ±4.0 °C, while precision was to 0.1 °C at all temperatures.

In order to observe low temperature phase transitions in all inclusion types, inclusions

were first super-cooled to around -50 °C for aqueous inclusions, -110 °C for carbon

dioxide bearing inclusions and -196 °C for methane inclusions, then reheated slowly at

1 °C/minute near expected phase transitions. During heating experiments, fluid

inclusion chips were heated at 5 °C/minute below 200 °C and 1 °C/minute above 200

°C.

Data collected included homogenization temperature of CH4 (Th CH4), melting

and homogenization temperatures of CO2 (TmCO2 and ThCO2, respectively), eutectic

temperature (TE), ice melting temperature (TmICE), clathrate melting temperature


48

(TmCLATH), total homogenization temperature of the inclusion (ThTOT ), and

decrepitation temperature (ThDECREP). The cycling technique of Goldstein and Reynolds

(1994) was employed during heating and freezing experiments in order to obtain

accurate phase transition temperatures. Salinity ( wt.% NaCl equiv.), bulk composition

and density were calculated using MacFlinCor (Brown and Hagemann, 1995) and the

equations of state for H2O-NaCl-KCl (Bodnar and Vityk, 1994) , and H2O-CO2-CH4-

NaCl and CO2-CH4 (Jacobs and Kerrick, 1981). The graphical methods of Swanenberg

(1979) and Thiery et al. (1994) were used to estimate the molar proportions of CO2 and

CH4. Laser Raman spectroscopy was used to quantify the content of the gas phases in

types I (methane), II (aqueous-carbonic) and III (carbonic) inclusions, and to identify

the nature of the daughter crystals. The relative proportions of CO2 and CH4 are

reported in mole percent (%) and density is reported in grams per cubic centimeter

(g/cm3).

4.1.3 Laser Raman Procedures

Laser Raman spectra of fluid inclusions were recorded at Geoscience Australia

on a Dilor SuperLabram spectrometer equipped with a holographic notch filter, 600

and 1800 g/mm gratings, and a liquid N2 cooled, 2000 x 450 pixel CCD detector. The

inclusions were illuminated with 514.5 nm laser excitation from a Melles Griot 543

argon ion laser, using 5 mW power at the samples, and a single 30 second accumulation.

A 100X Olympus microscope objective was used to focus the laser beam and collect the

scattered light. The focused laser spot on the samples was approximately 1 m in

diameter. Wave numbers are accurate to 1 cm-1 as determined by plasma and neon

emission lines. For the analysis of CO2, O2, N2, H2S and CH4 in the vapor phase, spectra

were recorded from 1000 to 3800 cm-1 using a single 20 second integration time per

spectrum. The detection limits are dependent upon the instrumental sensitivity, the

partial pressure of each gas, and the optical quality of each fluid inclusion. Raman

detection limits (Wopenka and Pasteris, 1987) are estimated to be around 0.1 mole

percent for CO2, O2 and N2, and 0.03 mole percent for H2S and CH4 and errors in the

calculated gas concentrations are generally less than 1 mole percent.

4.1.4 In Situ Fluid Inclusion Laser Ablation-ICP-MS Procedures

Selected single H2O-CO2 and H2O-rich fluid inclusions from types 2 and 3 veins

and quartz alteration were analyzed by laser ablation inductively coupled mass

spectrometry at the University of Leeds using an ArF 193nm Geolas Q Plus excimer


49

laser equipped with imaging optics (Gunther et al., 1997; Gunther et al., 1998). Double

polished thick section fluid inclusion wafers were glued onto glass slides and placed

into the sample chamber, which was evacuated of air then filled with He. Samples were

analyzed over a 90-second collection time, during which several inclusions could be

breached and analyzed. Dwell times were varied according to the number of elements

analysed in any given analysis, from 0.10 seconds (Na, Mg, K, Cu, Zn, Sr, Ag, Ba, Pb),

0.15 seconds (Na, K, Mn, As, Sb, Bi), 0.30 seconds (Au) and 0.40 seconds (Au). The

entire contents of the inclusion (liquid and solid daughter crystals) were transported to

the plasma as an aerosol using He carrier gas, then the samples were analyzed with an

Agilent 7500c quadrupole ICP-MS equipped with an octopole reaction cell. Fluid

inclusion analyses were calibrated using NIST SRM 610 and 612, an in-house EMPA

glass standard and glass capillaries filled with standard solutions. Signal data were

processed using a graphical user-interfaced software package developed at the

University of Leeds (Allan et al., 2005). In order to ensure that the results represented

the fluid inclusion contents and not host vein mineral concentrations, only spectra with

coincident Na and other cation peaks were processed. Inclusion-free quartz was check

analyzed for interference and produced no signal. The absolute element concentrations

of fluids in individual fluid inclusions were determined by charge balancing against the

H2O-NaCl equivalent chloride molality of each fluid inclusion population, as

determined by microthermometric heating/freezing experiments prior to the laser ICP-

MS analysis. Analytical precision for most elements is typically between 15 and 30%

RSD (relative standard deviation). Detection limits vary according to inclusion volume

but for most elements is 1 to 100µg/g. For a detailed description of the laser ICP-MS

analytical process refer to Allan et al. (2005).

4.2 Fluid Inclusion Petrography

4.2.1 Fluid Inclusion Classifications and Assemblages

Fluid inclusions are classified according to their origin as primary, secondary or

pseudosecondary (Roedder, 1979, 1984). Primary fluid inclusions are those whose

origins can be unequivocally tied to the formation of a crystal growth zone. Secondary

inclusions form as planar arrays or trails within healed microfractures that cross cut

crystal growth zones and grain boundaries. Pseudosecondary inclusions are essentially

identical to secondary inclusions except that they do not cross cut all mineral growth

zones or grain boundaries.


50

A fluid inclusion assemblage (FIA, Goldstein and Reynolds, 1994) comprises a

finely discriminated group of petrographically related inclusions that can be

demonstrated to have formed at the same time. The purposes of measuring fluid

inclusions within the context of FIA’s are twofold: (1) it allows for the identification of

post entrapment modifications to inclusions such as necking or thermal reequilibration,

which may render the microthermometric data uninterpretable, and (2) it is vital to the

identification of contemporaneously trapped immiscible fluids. The best examples of

FIA’s are secondary or pseudosecondary inclusions within a single healed fracture, or

primary inclusions within a crystal growth zone. For a more detailed description of fluid

inclusion petrography and the concept of fluid inclusion assemblages see Goldstein and

Reynolds (1994) and Reynolds (2003).

4.2.2 Fluid Inclusion Types

Fluid inclusions are abundant in quartz and calcite and occur as clusters within

single grains and along healed fractures both entirely within and cross-cutting grain

boundaries. Detailed petrography of fluid inclusions trapped in type 2 zoned quartz-

carbonate veins in Porphyry- and Mylonite- style mineralization samples, quartz-calcite

alteration associated with Contact-style mineralization, and type 3 quartz breccia veins

in Fracture-style mineralization samples revealed four inclusion types, which were

classified according to their phase ratios at room temperature: (I) CH4, (II) H2O-CO2,

(III) CO2-rich, and (IV) H2O-rich (Figure 4.1). These inclusion types were further

subdivided based on their behavior during heating and freezing runs and their

composition. Phase ratios of liquid water (LW), carbonic liquid (LC) and vapor at room

temperature (~22 °C) were estimated visually using the volumetric chart of Shepherd et

al. (1985). Microthermometry and laser Raman spectroscopy determined fluid inclusion

composition.

Type I CH4 inclusions are dark, generally rounded, and are always monophase at

room temperature. These inclusions are subdivided further based on their mode of

occurrence. Type Ia inclusions occur as clusters of small (~10 µm), negative crystal

shaped inclusions, and are restricted to the calcite selvedge of type 2 zoned quartz-

carbonate veins related to Stage I gold mineralization. Type Ib inclusions are ubiquitous

to both gold mineralizing events and occur as secondary trails of large (10-30 µm)

irregular inclusions, elongate in the trail orientation, in both type 2 and 3 veins. Laser

Raman analysis confirmed these as CH4±C2H6±C3H8 inclusions.


51

Type II H2O-CO2 inclusions are two- or three-phase at room temperature, and

are the most common inclusion type in both type 2 and type 3 veins and quartz-

carbonate alteration. They are typically small, ranging in size from 5-15 µm, and are

usually sub-rounded, except when they occur in calcite, where they are negative-crystal

shaped. Type II inclusions are trapped as clusters or internal trails that do not cross-cut

grain boundaries and are therefore considered pseudo-secondary. They typically display

constant phase ratios between CO2 and H2O of 0.3 to 0.4 in a single trail or cluster

within Type 2 veins, but have varied phase ratios, from 0.2 to 0.9 within a single trail or

cluster in Type 3 veins.

Type III CO2-rich inclusions are one- or two-phase at room temperature. They

are ovoid to sub rounded, typically occur in clusters or trails that cross cut grain

boundaries and are interpreted as secondary in origin. Inclusions range in size from 5-10

µm. Within a single trail or cluster, two-phase inclusions display constant phase ratios

around 0.9. Although these inclusions are described as H2O absent, they may contain up

to 20 percent invisible H2O in a thin film along inclusion walls (Roedder, 1972).


52

Figure 4.1 Fluid inclusion photomicrographs from representative samples at New Celebration. A. Clusters

of negative crystal shaped methane fluid inclusions in calcite from type 2 quartz-calcite veins. B.

Irregularly shaped, single phase (at room temperature) methane inclusions in quartz from type 2 quartz-

calcite vein. C. Cluster of type II aqueous-carbonic inclusions in quartz from type 2 veins. Two inclusions

contain a tiny rounded or triangular opaque daughter crystal. D. Transparent nahcolite (NaHCO3)

daughter crystal in type II aqueous-carbonic inclusions in quartz from type 2 vein. E. Type III CO2-

dominant inclusion from quartz-calcite alteration associated with Contact-style mineralization. F.

Secondary trail of type IV high salinity aqueous fluid inclusions in quartz from type 3 veins and quartz-

calcite alteration. In both vein types approximately 30% of inclusions contain tiny (<1 µm) rounded,

cubic or triangular opaque daughter crystals of unknown compositions and rarely (<5%) may contain

larger (up to 5 µm) ovoid or rod-shaped transparent nahcolite (NaHCO3, determined by laser Raman

analysis) daughter crystals.


53

Type IV H2O-rich aqueous inclusions are two-phase at room temperature. Some

inclusions in type 3 veins contain small amounts (less than 2.2 molal, (Ellis and

Golding, 1963; Roedder, 1984; Hedenquist and Henley, 1985) dissolved CO2,

evidenced by the formation of clathrate during freezing experiments and a double jerk

of the bubble during freezing cycles despite the absence of a separate liquid carbonic

phase at temperatures below the CO2 critical point. Distribution and occurrence of the

aqueous inclusions defined two inclusion populations: (1) irregularly shaped inclusions

containing rare opaque daughter minerals that were observed in either clusters or trails

within single crystals, which were interpreted as pseudosecondary, and (2) rounded to

ovoid shaped inclusions that occupied extensive fracture zones that cross cut quartz

grain boundaries and formed broad secondary trails. Inclusions of both populations are

typically very small (1-10 µm) and contain between 5 and 10 percent vapor.

4.3 Relative Timing Constraints

The relative timing relationships of fluid inclusion assemblages were

constrained based on cross-cutting relationships between host veins and structural

fabrics described in Chapter 3, and between cross-cutting relationships of various fluid

inclusion trails and clusters.

The earliest observed inclusion assemblages are interpreted to be those that are

located in the calcite margins of zoned type 2 quartz-calcite veins. These comprise type

I CH4 inclusions and type II H2O-CO2 inclusions, both of which form discrete clusters.

Assemblages of both fluid inclusion types formed in the calcite selvedge of zone quartz-

calcite veins associated with Porphyry style mineralization. Although there are no direct

cross-cutting relationships observed between assemblages of these fluid inclusion types,

the location of these assemblages in the calcite selvedge of the earliest studied vein

suggests that paragenetically they pre-date all other observed fluid inclusion

assemblages.

Assemblages of aqueous-carbonic and aqueous inclusion, which were trapped in

pseudosecondary trails and clusters in type 2 quartz-calcite veins within M1 porphyries,

are interpreted to post-date the assemblages trapped in the calcite selvedge of the same

veins as the zoning of these type 2 veins would suggest that the calcite selvedge formed

before the quartz.

Assemblages of aqueous-carbonic inclusions forming pseudosecondary trails

and clusters, and assemblages of carbonic only inclusions forming in M2 porphyry-


54

hosted type 3 veins are interpreted to post-date assemblages trapped in type 2 veins.

This is based on the observations that (1) M2 porphyries cross cut M1 porphyries, and

(2) type 3 veins cross cut D3NC foliation whereas type 2 veins are deformed by D3NC

foliation. The timing relationship between the aqueous-carbonic and the carbonic

assemblages cannot be determined as cross cutting relationships were not observed.

Assemblages comprising secondary trails of H2O-rich inclusions crosscut the aqueous-

carbonic and carbonic inclusion assemblages in both type 2 and 3 veins, and in quartz

and calcite alteration associated with Stage II Contact-style gold mineralization and are

therefore interpreted to post-date these assemblages. Secondary trails of CH4-rich

inclusions crosscut all other inclusion assemblages and are the latest inclusion

assemblages observed.

4.4 Microthermometry and Laser Raman Results

Microthermometric results were obtained for fluid inclusions within

petrographically defined fluid inclusion assemblages (Goldstein and Reynolds, 1994)

and are summarized in Table 4.1 and Figures 4.2 and 4.3. Where more than one

assemblage is measured, data are reported as ranges of means ± 1σ. All data are

contained in Appendices IV and V.

4.4.1 Type 1 CH4 Inclusions

Methane inclusions in calcite and quartz did not freeze at the lower temperature

limit of the Linkham stage (-196 °C). Primary inclusions in the calcite selvedge of type

2 veins formed a vapor bubble at low temperatures (-100 °C) ; upon warming these

inclusions homogenized to liquid between -76 °C and -73 °C (n=4). The composition of

these inclusions was not confirmed by laser Raman analysis. Secondary methane

inclusions in types 2 and 3 quartz veins also formed a vapor bubble at low temperatures,

but in contrast to the primary calcite-hosted inclusions, homogenized to liquid at around

-90 °C (n=5). Laser Raman analyses on secondary quartz-hosted inclusions confirmed

them as methane-dominant (95-100 mole % CH4) with minor N2 (up to 3 mole %) and

trace (1 mole %) C2H6 (ethane) and C3H8 (propane). These inclusions had densities of

0.26 ±0.00 g/cm3 (n=5) (Table 4.1).

4.4.2 Type 2 H2O-CO2 Inclusions

Aqueous-carbonic inclusions in the calcite selvedge of type 2 veins either

homogenized to liquid (ThTOT (L)) at 270 °C ± 1.0 °C (n=3) or decrepitated via


55

expansion of the vapor phase (ThCREP (V)) at 267 °C ± 0.4 °C (n=5). Melting of the

carbonic phase (TmCO2) ranged between -56.8 °C and -56.6 °C (n=9) (Fig. 4.2)

indicating that the gas phase comprised nearly pure CO2. Clathrate melting temperatures

(TmCLATH) ranged between 7.6 and 9.3 °C (n=9) (Fig. 4.3), giving calculated salinities

between 1.4 and 4.6 weight percent NaCl equivalent. In aqueous-carbonic inclusions

methane forms mixed hydrates with CO2. These hydrates have a higher Tm than CO2

clathrate, which gives a higher estimate when calculating salinity solely using clathrate

melting temperature (Collins, 1979), however, MacFlinCor (Brown and Hagemann,

1995), using the equations of state of Swanenberg (1979) and

Table 4.1 Summary of fluid inclusion microthermometric and laser Raman data from types 1, 2 and 3

veins. Salinities are reported as weight percent NaCl equivalent.

Type I CH4

Type II H2O-CO2-CH4-NaCl

Type III CO2-CH4

Type IV H2O

Type

1

Qua

rtz

Pseudosecondary TmCO2: -56.6 °C ThCO2: 28.1±1.0 °C XCH4: 0 mole% Bulk Density: 0.64 ± 0.05 g/cm4

Pseudosecondary H2O-NaCl TmICE: -7.8 °C ± 0.9 °C to -7.6 °C ± 1.2 °C ThTOT (L): 173.0 °C ± 29.2 °C to 192.0 °C ± 14.1 °C Salinity: 11.17 ± 1.59 to 11.39 ± 1.09 wt.% Bulk Density: 0.96 ± 0.2 to 0.97 ± 0.2 g/cm3

Type

2

Cal

cite

Pseudosecondary ThTOT (L): -76.4 – -73.0 °C

Pseudosecondary TmCO2: -56.73 °C±0.05 °C ThCO2: 29.58 °C±0.68 °C TmCLATH: 8.64 °C±0.53 °C ThDECREP (V): 267..23 °C ± 0.40 °C ThTOT (L): 269.58 °C ± 1.01 °C Salinity: 2.67 ± 0.99 wt.% XCO2: 16 ± 6 mole% XCH4: 0 mole% Bulk Density: 0.78± 0.04 g/cm3


56

Type I CH4


Type III CO2-CH4

Type IV H2O

Qua

rtz

Secondary ThTOT (L): -90.3 – -89.8 °C XCH4: 95-100 mole% XN2: 0-3 mole% XC2H6: 0-1 mole% XC3H8: 0-1 mole%

Pseudosecondary TmCO2: -59.50 °C ±1.55 °C to -56.60 ± 0.00 ThCO2: 11.95 ± 2.9 °C to 23.42 °C ± 0.96 °C TmCLATH: 6.0 - 9.8 °C ThDECREP (V): 226.4 °C ± 0.5 °C to 262.3 °C ± 15.2 °C ThTOT (L): 329.0 °C ± 0.4 ° C to 352.30 °C Salinity: 1.90 ± 1.18 to 5.92 ± 0.74 wt.% XCO2: 10±1 to 33 ± 13 mole% XCH4: 0 - 30 ± 1 mole% Bulk Density: 0.78 ± 0.04 to 0.94 ± 0.01 g/cm3

Solids: opaque mineral, nahcolite

Pseudosecondary TmICE: -8.7 ± 0.3 to 5.3 ±0.8 °C ThTOT (L): Salinity: 4.54 ± 1.32 to 12.50 ± 0.39 wt.% Secondary: TmICE -14.8 ± 0.1 ThTOT (L): Salinity: 18.41± 0.1

Qz-

cc a

ltn

Pseudosecondary TmCO2: -57.12 °C ± 0.46 °C to -56.6 °C ± 0.00 °C ThCO2: 14.98 °C ± 1.92 °C to 30.72 °C ± 0.04 °C TmCLATH: 6.7 °C ± 0.60 °C to 8.14 °C ± 0.17 °C ThDECREP (V): 247 °C to 276.60 °C ± 20.65 °C ThTOT (L-V): 296.95 °C ± 21.85 °C to 301.23 °C ± 10.78 °C Salinity: 3.63 ±0.31 to 5.73 ± 1.01 wt.% XCO2: 48 ± 17 to 53 ± 28 mole% XCH4: 0 – 1 mole% Bulk Density: 0.65 ± 0.06 to 0.90 ± 0.05 g/cm3

Pseudosecondary H2O-NaCl>>CO2 TmICE: -5.7 °C ± 1.9 °C to -2.6 °C ± 2.5 °C ThTOT (L): –212.7 °C ± 20.1 °C Salinity: 3.06 ± 1.16 to 8.65 ± 2.60 wt.% Secondary H2O-NaCl-CaCl2 TmICE: -21.1°C ± 1.7 °C to -19.0 °C ± 3.1 °C ThTOT (L): 89.0 °C ± 13.5 °C to 101.9 °C ±22.8 °C Salinity: 18.4 ± 0.1 to 22.3 ± 0.9 wt.% Bulk Density: 1.12 ± 0.02 to 1.16 ± 0.01g/cm3

Pseudosecondary H2O-NaCl TmICE: -5.7 ± 1.9 to -3.1 ± 1.8 °C ThTOT (L): 100.5 °C ± 10.1 °C Salinity: 6.85 ± 1.20 to 2.67 wt.%


57

Type I CH4


Type III CO2-CH4

Type IV H2O

Type

3

Pseudosecondary TmCO2: -57.82 °C ± 0.04 to -56.6 °C ThCO2: 14.90 °C ± 0.83 °C to 29.20 °C ± 2.08°C TmCLATH: 7.00 °C ± 0.10 ° C to 8.60 °C ± 0.41 °C ThDECREP (V): 247.0 °C to 276.6 ± 20.65 °C ThTOT (L-V): 297.0 °C ± 21.90 to 301.23 °C ± 10.78°C Salinity: 4.97 ±0.54 to 5.68 ± 0.17 wt.% XCO2: 16± 3 to 26 ± 8 mole% XCH4: 0 – 1 mole% Bulk Density: 0.74 ± 0.11 to 0.95 ± 0.01 g/cm3

Primary & pseudosecondary TmCO2: -57.0 ± 0.2 to -56.6 °C ThCO2: 10.3 °C ± 3.1 °C to 28.1 °C ± 1.0 °C XCH4: 0 – 3 mole% Bulk Density: 0.72 ± 0.03 to 0.85 ± 0.05 g/cm3

Pseudosecondary TmICE: -5.7 ± 1.9 to -3.1 ± 1.8 °C ThTOT (L): 100.5 °C ± 10.1 °C Salinity: 6.85 ± 1.20 to 2.67 wt.% Secondary H2O-NaCl-CaCl2 TmICE: -19.0°C ± 3.1 °C ThTOT (L Salinity: 21.0 ± 1.9 wt % Bulk Density:

Thiery et al. (1994) take the molar proportion of CH4 into account when calculating

salinity therefore providing an accurate representation of salinity in the system H2O-

CO2-NaCl-CH4. The CO2 phase homogenized to liquid between 29 and 31 °C (n=9)

(Fig. 6). Inclusions contained between 8 and 27 mole percent CO2 and have calculated

bulk densities ranging between 0.73 and 0.86 g/cm3 (Table 4.1). In both types 2 and 3

veins and quartz-calcite alteration most of the aqueous-carbonic inclusions decrepitated

before final homogenization. In type 2 veins, inclusions invariably decrepitated via

expansion of the vapor phase at temperatures ranging from 226 °C ± 1 °C to 277 °C ± 0

°C. In type 3 veins, fluid inclusions decrepitated by expansion of either the liquid or

vapor phase at temperatures between 247 °C ± 0.00 °C and 277 °C ± 21 °C. In one

assemblage in quartz-calcite alteration, inclusions decrepitated by expansion of either

the liquid or the vapor phase at 186 °C ± 0 °C. Where inclusions homogenized,

homogenization


58

Figure 4.2 A. CO2 melting temperature (Tm CO2) versus CO2 homogenization temperature (Th CO2 (L)) of

type II aqueous inclusions in calcite from type 2 veins, in quartz from type 2 veins, in quartz-calcite

alteration and in quartz from type 3 veins. Inclusions in quartz from Stage I-related type 2 veins display a

much wider spread of values than those in quartz-calcite alteration and quartz from type 3 veins

associated with Stage II gold mineralization. While all fluids are relatively low in CH4, Stage II fluids

contain significantly less CH4 than Stage II and have a higher density. Contours of XCH4 and VCAR (molar

volume of the carbonic phase), critical curve, and liquid-solid-gas (LSG) univariant curve from Neumayr

and Hagemann (2002) after Thiery et al. (1994). Histograms of ThCO2 and TmCO2 in B. type II aqueous-

carbonic inclusions in calcite from type 2 veins; C. type II aqueous-carbonic inclusions in quartz from

type 2 veins; D. type II aqueous-carbonic inclusions in quartz-calcite alteration (grey) and type 3 veins

(white); E. type III carbonic inclusions from quartz in type 1 veins (hatch), quartz-calcite alteration (grey)

and type 3 veins (white). aq=aqueous, cb=carbonic, qz=quartz, cc=calcite, altn=alteration, pp=porphyry,

ct=fracture, ct=contact, my=mylonite.


59

Figure 4.3 Histograms of TmCLATH or TmICE for A) primary type II aqueous-carbonic inclusions in calcite

from type 2 veins; B) type II aqueous-carbonic inclusions in quartz from type 2 veins; C) type II aqueous-

carbonic inclusions in quartz-calcite alteration (grey) and type 3 veins (white); D) type IV aqueous

inclusions with trace CO2 in quartz-calcite alteration (grey) and type 3 veins (white); E) type IV low

salinity aqueous inclusions without CO2 in type 1 veins (hatch), quartz in type 2 veins (black)and type 3

veins (white); and F) secondary type IV high salinity aqueous inclusion from quartz in type 2 veins

(black), quartz-calcite alteration (grey) and type 3 veins (white). Qz-cc altn=quartz-calcite alteration.

occurred between 329 °C ± 0.4 °C and 352 °C in inclusion assemblages in type 2 veins,

297 °C ± 22 °C and 301 °C ± 11 °C in type 3 vein assemblages and at 304 °C ± 17 °C in

quartz-calcite alteration. Melting of the carbonic phase (TmCO2) in inclusions from type

2 veins occurred at slightly lower temperatures (-59.5 °C ± 1.6 °C to -56.6 °C ± 0.0 °C)

than inclusions in quartz-calcite alteration and type 3 veins (-57.8 °C ± 0.04 °C to -56.6

°C) (Fig. 4.2), which indicates they contained higher concentrations of other gases, such

as methane. Laser Raman analysis, which identified up to 39 mole% CH4 in aqueous-

carbonic inclusions from type 2 veins, confirmed this (Table 4.1). Homogenization of

the carbonic phase to liquid occurred from 12.0 °C ± 1.6 °C to 23.4 °C ±1.0 °C in

inclusions in type 2 veins and 14.9 °C ± 0.8 °C to 30.7 °C ± 0.04 °C in inclusions

hosted in quartz-calcite alteration and type 3 veins (Fig. 4.2, Table 4.1). Fluid densities,

calculated using the graphical methods of Swanenberg (1979) ranged between 0.65

g/cm3 ± 0.06 g/cm3 and 0.95 g/cm3 ±0.01 g/cm3, although inclusions in type 2 veins had

a narrower range (Table 4.1). Final clathrate melting temperatures ranged between 6.9

C° ± 0.4 °C and 9.1 °C ± 0.6 °C (Fig. 4.3) in assemblages from both vein types and


60

quartz-calcite alteration, equating to average salinities between 1.9 ± 1.2 weight percent

NaCl and 5.9 ± 0.7 weight percent NaCl equivalent, calculated using MacFlinCor

(Brown and Hagemann, 1995) and the equation of state for H2O-CO2-CH4-NaCl (Jacobs

and Kerrick, 1981). Where recorded, eutectic temperatures, which were difficult to

measure given the small size and dark color of the inclusions, were around -85 °C,

indicating the presence of cations other than Na+.

Type II inclusions commonly contained nahcolite and/or opaque daughter

crystals. Neither of these minerals showed any change in their shape during heating

experiments.

4.4.3 Type III CO2-Rich Inclusions

In assemblages of CO2-rich inclusions from type 3 veins, melting temperatures

of the carbonic phase ranged from -57.0 °C ± 0.2 °C to -56.6 °C (Fig. 4.2) indicating

that the inclusions were essentially almost pure CO2. Homogenization temperatures

(ThCO2) ranged from 10.3 °C ± 3.1 °C to 28.1 °C ± 1.0 °C (Fig. 4.2), although most of

the inclusions returned ThCO2 values > 18 °C. Calculated densities of the carbonic phase

varied from 0.64 g/cm3 ± 0.05 g/cm3 to 0.85 g/cm3 ±0.05 g/cm3. Methane contents

ranged between 0 and 3 mole percent CH4 (Table 4.1).

4.4.4 Type IV H2O-Rich Inclusions

Assemblages of aqueous inclusions containing trace dissolved CO2 (as

evidenced by the formation of clathrate during freezing measurements) in quartz-calcite

alteration and type 3 veins displayed eutectic temperatures (TE) between -20 °C and -24

°C indicating that the fluids were H2O-NaCl dominated (Borisenko, 1977; Crawford,

1981). All but three inclusions homogenized to liquid between 140 °C and 267 °C. The

remaining inclusions decrepitated via expansion of the liquid phase at 229 °C and 236

°C or via expansion of the vapor phase at 252 °C. Ice melting temperatures ranged

between -5.7 °C ± 1.9 °C and -2.6 °C ±2.5 °C (Fig. 4.3). The presence of CO2 affects

the salinity measurements, as low levels of CO2 will depress the ice melting temperature

by up to 1.5 °C (Hedenquist and Henley, 1985), however, clathrate melting

temperatures in the absence of liquid CO2 invalidate salinity calculations using TmCLATH

(Diamond, 1992). Calculated apparent salinities (maximum salinity) of type IIb

inclusions ranged between 3.06 ± 1.16 weight percent NaCl equivalent and 8.65 ± 2.60

weight percent NaCl equivalent and fluid densities ranged between 0.89 ± 0.04 g/cm3

and 0.91 ± 0.9 g/cm3 (Table 4.1).


61

Pseudosecondary aqueous inclusions without dissolved CO2 also had eutectic

temperatures around -20 °C, indicating that these fluids were also within the H2O-NaCl

system. Ice melting temperature of inclusions in type 2 quartz veins ranged between -

8.7 °C ± 0.3 °C and -5.3 °C ± 0.8 °C (Fig. 4.3) correlating to calculated salinities

between 4.54 ± 1.32 and 12.5 ± 0.39 weight percent NaCl equivalent and densities

between 0.85 ± 0.08 g/cm3 and 0.97 ± 0.02 g/cm3. In type 3 quartz veins, final

homogenization occurred at much lower temperatures, at 100.5 °C ± 10.1 °C, in the

only assemblage upon which ThTOT was collected. Ice melting temperatures ranged

between -5.7 °C ± 1.9 °C and -3.1 °C ± 1.8 °C (Fig. 4.3). Calculated salinities ranged

between 6.85 ± 1.20 to 6.03 ± 2.67 weight percent NaCl equivalent. densities in all

assemblages clustered around 0.97 ± 0.01 g/cm3 (Table 4.1).

Secondary H2O-rich inclusions in both types 2 and 3 veins had eutectic

temperatures around -55 °C placing them in the H2O-NaCl-CaCl2 system (Borisenko,

1977; Crawford, 1981). Inclusions in all assemblages homogenized to liquid at

temperatures between 89.0 °C ± 13.5 °C and 101.9 °C ± 22.8 °C. Ice melting

temperatures in type 3 veins ranged between -21.1 °C ± 1.7 and -17.7 °C ± 1.7 °C, but

were slightly higher in type 2 veins(Fig. 4.3). Calculated salinities ranged between 18.4

± 0.1 weight percent NaCl equivalent and 22.3 ± 0.9 weight percent NaCl equivalent

and densities between 1.12 g/cm3 ± 0.02 g/cm3 and 1.16 g/cm3 ± 0.01 g/cm3 (Table

4.1).

4.4.5 Interpretation of Laser Raman and Microthermometry Results

4.4.5.1 Evidence for Fluid Immiscibility

Given the broad two-phase field in the H2O-CO2-NaCl system (Takenouchi and

Kennedy, 1965; Gehrig et al., 1980), it is important to determine whether the different

fluid inclusion assemblages observed at New Celebration could have resulted from

phase immiscibility processes. This may occur as a consequence of sudden pressure

reduction due to fault movement (Cox et al., 1995), fluids ascending to higher crustal

levels or fluid interaction with carbon (Naden and Shepherd, 1989). Fluid inclusions in

the CO2-H2O system were either trapped from a homogeneous fluid in the single phase

field, or they were trapped from a heterogeneous fluid in the two-phase field (Diamond,

2001). In theory, the state of entrapment of cogenetically trapped inclusions should be

readily distinguishable by applying the principle of uniformity of phase volume

proportions (Sorby, 1858; Roedder, 1984). Inclusions trapped contemporaneously in


62

the single phase field should have similar compositions, bulk molar volumes and phase

proportions. Conversely, inclusions trapped in the two phase field will show highly

variable bulk compositions, bulk molar volumes and phase proportions (Loucks, 2000;

Diamond, 2001).

Within individual fluid inclusion assemblages, Type II inclusions in type 2 veins

show very little variation of phase proportions, bulk composition or molar volume.

Inclusions within individual assemblages do not display liquid-rich and vapour-rich

end-members, suggesting that phase separation did not occur (c.f. Diamond, 2001) and

was not a factor in the development of Stage I gold mineralization.

Phase proportions, bulk compositions and molar volumes of Type II inclusions

in Stage II mineralisation show more diversity within a single cluster or trail than those

trapped in Stage I. In locations where both liquid-rich and vapor-rich fluid inclusions

occur in a cogenetic assemblage, Ramboz et al. (1982) have outlined three criteria to

determine whether phase separation has taken place. These are:

(1) “The two types of inclusions must occur in the same regions of the same

sample” i.e. the same internal trail or three-dimensional cluster, “and there must

be good evidence for their contemporaneous trapping”.

(2) “The two types of inclusions must homogenise at the same temperature, or more

realistically within the same range of temperature (because trapping is not an

instantaneous and strictly isothermal-isobaric process). One type must

homogenize into a liquid (V + L→L), the other must homogenize into a vapor

(V + L→V)”.

(3) “Upon heating, the pressures in the two types of inclusions before

homogenization are different (because of the difference in their compositions

and densities). The pressures reach the same value (trapping pressure) at

homogenization temperature. Therefore, if one inclusion type decrepitates

before homogenizing, the other type must behave similarly.”

Most inclusion assemblages in type 3 veins and quartz-calcite alteration

contained only liquid-rich aqueous-carbonic inclusions, which could possibly represent

the parental, unmodified hydrothermal fluid (c.f. Robert and Kelly, 1987), however, at

least six assemblages displayed liquid and vapor-rich inclusions within the same trail or

cluster. Aqueous-carbonic inclusion assemblages from Stage II-related type 3 quartz

veins and quartz-calcite alteration did display some evidence for local fluid


63

immiscibility including: (a) liquid and vapor-rich end members in some coeval

assemblages, (b) variable bulk compositions and molar volumes within an individual

inclusion assemblage, (c) total homogenization into liquid and vapor at the same

temperature of at least some of the inclusions within a single fluid inclusion assemblage

and (d) decrepitation of both liquid- and vapor-rich inclusions at similar temperatures

within any given assemblage.

Many of the vapor-rich aqueous-carbonic fluid inclusions decrepitated,

However, most vapor-rich inclusions homogenized to vapor before decrepitating. The

observation that several, albeit limited assemblages, display vapor and liquid-rich end

members, and that many vapor-rich fluid inclusions homogenized into vapor before

decripitation suggests that, at least locally, the fluid inclusions were trapped during fluid

immiscibility, thereby likely facilitating the precipitation of pyrite and gold during Stage

II mineralization.

4.4.5.2 Trapping Conditions

In hydrothermal systems where phase separation has not taken place, pressures

derived from homogenization temperatures represent minimum values, and independent

pressure and temperature estimates must be applied to determine the trapping conditions

of these fluids (cf. Roedder, 1984). Where phase separation has occurred,

homogenization temperatures represent trapping temperatures. The lack of evidence for

phase separation in fluid inclusion assemblages means that independent pressure

estimates must be applied in order to constrain the trapping conditions. At New

Celebration independent pressure estimates are provided by: (a) phengite geobarometry

on sericite alteration that is in equilibrium with sulfides of Stage I gold mineralization in

the Southern Ore Zone, and (b) regional greenschist facies metamorphism interpreted to

be broadly contemporaneous with orogenic gold mineralization in the Kalgoorlie-

Norseman corridor (McNaughton et al., 1990; Witt, 1991).

The underground Southern Ore Zone produced approximately 140,000 oz of

gold from M1 porphyry and was the primary source of Stage I gold at New Celebration

(Newcrest Mining Limited Internal Report, 2000). Phengite geobarometry on gold-

related sericite alteration constrains formation pressures to between 3.2 and 4.2 kbars

(Williams, 1994). Recent metamorphic studies in the eastern Yilgarn craton by

Goscombe et al. (2007; 2009) revealed that preceding hydrothermal alteration and

orogenic gold mineralization a regional M2 metamorphism linked to compression and


64

minor crustal thickening was characterized by temperatures of 300-500°C and pressures

of 3.5-4.0 kbars. Based on equilibrium petrographic relationships between gold-hosting

pyrite, type 2 quartz-calcite veins and S3NC fabrics, the timing of Stage I gold

mineralization at New Celebration is interpreted to be syn- to immediately post-peak

metamorphism, contemporaneous with peak metamorphic conditions (Nichols, 2003),

therefore the regional metamorphic conditions described by Goscombe et al. (2007;

2009) can be used as a maximum P-T constraint on gold mineralization at the New

Celebration gold deposits.

Figure 4.4 illustrates representative median isochores calculated from fluid

inclusions trapped during the different hydrothermal events at New Celebration.

Isochores were constructed in MacFlinCor (Brown and Hagemann, 1995) using freezing

point depression, volume fraction vapor and ThTOT , and the equations of state of Bodnar

and Vityk (1994) for H2O-NaCl-(KCl) inclusions, TmCO2, volume fraction vapor at

TmCO2, ThCO2, and the equations of state of Thiery et al. (1994) and Swanenberg (1979)

for CO2-CH4 inclusions, and TmCO2, TmCLATH, ThCO2, ThTOT and the equations of state

of Thiery et al. (1994) and Swanenberg (1979) for H2O-CO2-CH4-NaCl inclusions.

Minimum trapping pressures for assemblages where phase immiscibility was not

demonstrated were derived from the intersection of the minimum homogenization

temperature of an inclusion type with its respective representative median isochore:

maximum P-T conditions are constrained by independent pressure estimates. At New

Celebration these are imposed by the limits of upper greenschist facies regional

metamorphism (c.f. Goscombe et al., 2007; 2009) and an independent P-T estimate for

Southern Ore Zone mineralization derived from the chlorite solid-solution

geothermometer and phengite geobarometer (Williams, 1994). In assemblages where

phase separation is demonstrated, homogenization temperatures represent trapping

conditions.

Using pressures derived from minimum homogenization temperatures of

different inclusion types, and the independent geothermobarometric constraints outlined

above, an approximate P-T-t path for the hydrothermal fluids circulating through the

Boulder-Lefroy fault segment, thus constraining the fluid evolution of the New

Celebration gold deposits, is illustrated in figure 4.5. Pressure-temperature boxes

illustrated in figure 4.5 were constructed using homogenization temperatures derived

from microthermometric analysis and independent pressure estimates, described above.


65

Figure 4.4 P-T diagram showing representative median isochores from different fluid inclusion types in

types 2 and 3 veins and quartz-calcite alteration. (A) secondary late methane inclusions in all vein types;

(B) primary aqueous-carbonic inclusions in calcite from type 2 veins: (C), Stage II pseudo-secondary

aqueous-carbonic inclusions from type 3 veins and quartz-calcite alteration; (D) Stage I pseudosecondary

aqueous-carbonic inclusions from type 2 veins; and (E) late secondary aqueous inclusions from all vein

types. Minimum trapping pressures for assemblages where phase immiscibility was not demonstrated

were derived from the intersection of the minimum homogenization temperature of an inclusion type and

its respective representative isochore, shown on the diagram as lines with filled circles at each end.

Maximum P-T conditions are constrained by independent pressure estimates. At New Celebration these

are imposed by the limits of upper greenschist facies regional metamorphism (c.f. Goscombe et al., 2007;

2009) and an independent P-T estimate for Southern Ore Zone mineralization derived from the chlorite

solid-solution geothermometer and phengite geobarometer (Williams, 1994). The minimum

homogenization temperature of aqueous-carbonic fluid inclusions from quartz in type 2 veins, associated

with Stage I gold mineralization, constrains the minimum trapping pressure of these inclusions to

approximately 3.2 kbars. Maximum pressure constraints imposed by the limits of regional metamorphism

constrains the upper temperature of formation of Stage I mineralization to 390 °C. Stage II mineralization

formed at similar temperatures, but much lower pressures, with minimum formation conditions of 300 °C

and 1 kbar. The representative isochores for late secondary methane inclusions (A) and late secondary

aqueous inclusions (F) show P-T relationships outside of the range for gold mineralization, indicating that

these inclusions formed in a different P-T environment and are unlikely to be gold related.

The earliest observed aqueous-carbonic inclusions in calcite from type 2 quartz-

calcite veins, and by inference, the early carbonic inclusions within the same calcite

selvedge, formed between 270 °C and 500 °C at 1 to 3 kbars assuming lithostatic fluid

pressures. The minimum homogenization temperature of aqueous-carbonic fluid

inclusions from quartz in type 2 veins associated with Stage I gold mineralization (330

°C), constrains the minimum trapping pressure of these inclusions to approximately 3.2


66

kilobars. Maximum pressure constraints imposed by the limits of regional

metamorphism constrains the upper temperature of formation of Stage I mineralization

to 390 °C. Stage I gold mineralization is therefore interpreted to have formed beween

330 °C and 390 °C at pressures between 3.2 and 4.0 kbars. This corresponds to a

paleodepth of 10-15km (Brown and Hagemann, 1995), assuming lithostatic conditions

and lies between the mesozonal and hypozonal classifications of Gebre-Mariam et al.

(1995) and Groves et al. (1998).

In assemblages where phase separation has taken place homogenization

temperature represents trapping conditions. Homogenization temperatures of aqueous-

carbonic inclusions from quartz in type 3 veins related to Stage II mineralization

constrain minimum trapping pressures to 0.8 kbars. Upper limits for the boiling

assemblages are constrained by homogenization temperatures around 320 °C, which

correlates to trapping pressures of 1.2 kbars. For Stage II assemblages where boiling

was not demonstrated, maximum trapping pressures can only be constrained by regional

metamorphism, giving a maximum trapping pressure of 3.2 kbars. Stage II

mineralization is therefore interpreted to have formed at temperatures between 280 °C

and 320 °C and pressures between 0.8 and 3.2 kbars, which corresponds to crustal

depths between 4 and 10 kilometers(Brown and Hagemann, 1995) at lithostatic

conditions. In conjunction with fluid inclusion evidence for local fluid immiscibility,

this variation in pressure may represent pressure fluctuations due to fault valve

seismogenic cyclic fault valve behavior (Sibson et al., 1988; Sibson, 2004) in a brittle

tectonic regime.

Carbonic inclusions, interpreted as trapped during the final phases of Stage II

gold mineralization, have estimated trapping conditions between 280 °C and 360 °C and

0.8 to 1.6 kbars. High salinity aqueous inclusions, and methane inclusions trapped in all

vein types and quartz-calcite alteration formed at temperatures around 100-180 °C and

pressures estimated to range between 0.4-1.0 kbars.The representative isochores for late

secondary methane inclusions (A) and late secondary aqueous inclusions (F) show P-T

relationships outside of the range for gold mineralization, indicating that these

inclusions formed in a different P-T environment and are unlikely to be gold related.


67

Figure 4.5 Pressure-temperature diagram illustrating the P-T conditions of formation of different fluid

inclusion assemblages in various vein types, the P-T path through time, the likely pressure constraints

imposed by peak metamorphism (from Spears, 1995) and the independent P-T estimate of Williams

(1994) for Southern Ore Zone mineralization at New Celebration derived from the chlorite solid-solution

geothermometer and phengite geobarometer. Interpretation of the P-T conditions recorded by the different

fluid inclusion assemblages indicates a protracted and complex fluid and tectonic history for the BLFZ.

Early fluids were emplaced in the fault at or around peak metamorphism; Stage I gold mineralization

formed post-peak metamorphism at high temperatures and pressures. Stage II mineralization formed

during a period of waning temperature and fluctuating pressure, possibly induced by fault valve behavior.

Late fluid assemblages (highly saline aqueous fluids, and methane-dominated fluids) were emplaced

during a period of low temperature and pressure, likely during uplift and erosion of the orogen

4.4.5.3 Fluid Mixing

The distribution of data in a conventional bivariate plot of homogenization

temperature (Th TOT) versus salinity ( wt.% NaCl equiv.) for fluid inclusions trapped

during both stages of gold mineralization (Fig. 4.6) does not indicate that fluid mixing

was a significant fluid process (cf. Wilkinson, 2001). The relationship expressed in

Figure 4.6, however, does not take into account the possibility of mixing aqueous or

aqueous-dominated fluids with one or more gaseous fluids. Fluid inclusion evidence

indicates the presence of a CO2 dominated fluid in type 3 quartz veins. These inclusions

may reflect partial mixing between aqueous-carbonic ore fluids and CO2-dominated

fluids; however, the paragenetic relationship between the H2O-CO2 and CO2-rich

inclusion populations is unclear. The source of the CO2-dominated fluid is

unconstrained, however, the close spatial association of the New Celebration deposit to

felsic porphyry dikes points towards a potential granite source at depth


68

Figure 4.6 Salinity (wt. % NaCl equiv.) versus total homogenization temperature (ThTOT) for types II

(H2O-CO2- filled symbols) and IVa (H2O-NaCl – open symbols) fluid inclusions from Stage I (A) and

Stage II (B) gold mineralization. Type IVb (high salinity H2O-NaCl-CaCl2 – asterisks) fluid inclusions

are included on both plots for comparison. There is no evidence for either isothermal fluid mixing or

dilution of the ore fluids with surface fluids in either Stage I or Stage II gold mineralization. The late,

highly saline aqueous fluids form a discrete population and do not appear to be related to the earlier

fluids. However, these diagrams do not take into account the possibility of mixing aqueous or aqueous-

carbonic fluids with one or more gaseous fluids. Boiling and mixing lines from Wilkinson (2001).

(cf. granite underlying the area south of Kalgoorlie, Stolz et al., 2004). This granite, if

contemporaneous with ore formation, could exsolve highly oxidized hot CO2-rich fluids

that mixed with the ore fluids ascending the BLFZ.

There is also fluid inclusion evidence for methane-dominated fluids within the

BLFZ hydrothermal system. Fluid mixing between CH4 and CO2-bearing ore-fluids


69

could trigger phase immiscibility (Naden and Shepherd, 1989) by pushing the solvus

towards higher temperatures and pressures and increasing the two-phase field in the

H2O-CO2 system (McCuaig and Kerrich, 1998). If this was the case, the ore-related

H2O-CO2 fluid inclusions should be expected to contain higher concentrations of CH4,

however, except for rare inclusions, the mole fraction of CH4 in H2O-CO2 inclusions

was less than 0.03.

4.5 LA-ICP-MS Results

Mixed aqueous-carbonic and aqueous inclusions from types 2 and 3 veins, and

quartz-calcite alteration were analyzed by laser ablation inductively coupled plasma

mass spectrometry (LA-ICP-MS) to determine the metal concentrations in mineralizing

and non-mineralizing fluids. Inclusions of all fluid types contained Na, K, Ca, Mg and

Fe as major components, and contained trace to minor concentrations of other metals

such as Cu, Pb, Zn, As, Ag and Au. Element ratios in mixed inclusions with daughter

minerals did not show any systematic variations from those without daughter minerals.

Comparisons of element ratios (to Na, figure 4.7) and concentrations (figure 4.8)

between the different inclusion types revealed a number of differences. Aqueous-

carbonic inclusions in type 2 veins (n=174) were composed of fluids characterized by

Na>Ca>K> Mg and K/Ca <1 (table 4.2), whereas inclusions in type 3 veins (n=95) and

quartz-calcite alteration associated with Contact-style mineralization (n=88) were

characterized by Na>Mg>K>>Ca fluids and K/Ca >1 (table 4.2). Low salinity aqueous

inclusions in type 3 veins were Na>>K>Mg; Ca was not analysed in these inclusions.

Late, high salinity aqueous inclusions, reported in all vein types and quartz-cc alteration

were Na>K>>Ca, with only minor Mg.

Metal concentrations were generally low in all inclusions from both vein types,

and were commonly below detection although mixed inclusions in all hosts contained

up to 163 ppm Cu, 75 ppm Zn and 43 ppm As (c.f. Olivo et al., 2006; Pudack et al.,

2009). Bar plots of mean element ratios (figure 4.9) and concentrations (figure 4.10)

illustrate the differences between the fluid types. Analyses of stage I gold-related

aqueous-carbonic fluid inclusions from type 2 veins returned lower values than Stage II

aqueous-carbonic fluids from type 3 veins and quartz-calcite alteration for all metals

except Cu and Sn. Aqueous-carbonic fluids in quartz-calcite alteration (Stage II,

Contact style) returned lower values for all metals except Sn than the same fluids in

type 3 veins (Stage II, Fracture style). Low salinity aqueous fluids in type 3 veins


70

returned similar metal ratios and concentrations to aqueous-carbonic fluids in the same

veins. Interestingly, high salinity aqueous inclusions, which are interpreted to post-date

gold mineralization, returned Cu concentrations up to 800 ppm and Ag up to 48 ppm.

4.5.1 Gold

Gold was analysed separately from other elements in order to increase the dwell

time (to 0.30 or 0.40 seconds), which serves to reduce background interference and

decreases limits of detection (LOD). In many inclusions gold was below detection,

however, individual aqueous-carbonic inclusions contained up to 51 ppm Au. Average

Au concentrations (figure 4.10) from both vein types and quartz-calcite alteration

showed little variation, with mixed inclusions returning mean values of 4.76 ppm (type

2 veins, n=76), 5.12 ppm (type 3 veins, n=40) and 6.26 ppm (quartz-calcite alteration,

n=21).

The Au values reported from both types 2 and 3 veins and quartz-calcite

alteration are consistent with the experimental work of Mikucki and Ridley (1993) and

Mikucki (1998), who determined that at temperatures between 300 °C and 550 °C, gold

transported as a bisulfide complex (Au(HS)2-) could have solubilities exceeding 10-

10,000 ppb Au. They also exceed the minimum 5 ppb Au concentration required to

form an ore fluid capable of forming a gold deposit (Heinrich et al., 1989).


71

Figure 4.7 Bar graph of mean Mg, K and Ca ratios (to Na) of New Celebration fluids illustrating the

differences between Stages I and II gold mineralization, and post mineralization fluids.

Figure 4.8 Bar graph of mean Mg, K and Ca concentrations of New Celebration fluids illustrating the

differences between Stages I and II gold mineralization, and post mineralization fluids.


72

Figure 4.9 Mean ratios of some metals (to Na) in fluid inclusions from the New Celebration deposit

illustrating the difference in metal abundances between Stages I and II gold and post-Au fluids

Figure 4.10 Mean ratios of some metals (to Na) in fluid inclusions from the New Celebration deposit

illustrating the difference in metal abundances between Stages I and II gold and post-Au fluids


73

4.5.2 Interpretation of In Situ Laser Ablation ICP-MS Results

4.5.2.1 Potential Fluid Sources

Based on the characterization of sedimentary-derived brines as Na-Ca

dominated (Taylor et al., 1983; Haynes and Kesler, 1987; Haynes, 1988), and magmatic

fluids as Na-K dominated (Roedder, 1971; Kilinc and Burnham, 1972; Eastoe, 1978;

Burnham, 1979; Wilson et al., 1980; Whitney et al., 1985; Quan et al., 1987), Haynes

and Kesler (1988) suggested that K/Ca could be used to evaluate magmatic fluid

contributions to ore mineralization. They suggested that K/Ca ratios >1 indicated a

dominantly magmatic fluid source, or a fluid that had equilibrated with granitic rocks,

whereas K/Ca ratios <1 indicated a dominantly non-magmatic, basinal-derived fluid

source. At New Celebration Stage I-related fluid inclusions from type 2 quartz-

carbonate veins have K/Ca ratios < 1, whereas Stage II-related fluid inclusions trapped

in quartz-calcite alteration and type 3 quartz veins, and high salinity aqueous inclusions

which are trapped in the same veins but post-date gold mineralization have K/Ca ratios

>1. This indicates that a switch in fluid sources may have occurred between the Stage I

and Stage II gold mineralizing events, from a non-magmatic, likely metamorphic, fluid

that circulated during Stage I gold mineralization, to dominantly magmatic fluids during

Stage II.

4.6 Comparisons with Other Hydrothermal Systems

Hydrothermal fluids recorded at New Celebration are for the most part similar to

fluids reported from orogenic deposits around the world. Goldfarb et al. (2005, and

references therein) reported that the majority of orogenic lode gold deposits formed

from near-neutral pH fluids containing 4-30 mole percent CO2 with salinities ranging

between 3 and 12 weight percent NaCl equivalent. Most fluid inclusions from gold-

bearing veins contained some CH4±N2, with CH4 and/or N2 concentrations ranging from

trace amounts to concentrations greater than the total amount of CO2. Various workers

have reported highly saline aqueous fluids from orogenic lode gold deposits, although

their relationship to mineralization remains contentious. Some highly saline fluids (e.g.

Sigma, Robert and Kelly, 1987; Victory-Defiance, Clark et al., 1989) are considered to

be the end-members of fluid unmixing. Others (e.g. Abitibi subprovince, Boullier et al.,

1998) clearly post-date gold mineralization and are interpreted to represent late shield

brines (Guha and Kanwar, 1987). Methane dominant fluids are less common but have


74

been observed in a number of deposits in the Yilgarn craton, such as the Oroya lodes at

Golden Mile (Ho, 1987), Wiluna (Hagemann et al., 1996), Mt Charlotte (Mernagh,

1996) and Victory (Polito et al., 2001). For the most part, the presence of methane-rich

fluids is attributed to carbonaceous wall rocks either hosting or adjacent to the deposits,

however, others, such as New Celebration and Junction, have no associated

carbonaceous units. Polito et al. (2001) considered Fischer-Tropsch reactions between

light hydrocarbons and wall rock Fe-oxides under reducing conditions to be the

mechanism by which the methane-rich inclusions formed at Junction. Alternatives

include phase immiscibility (Naden and Shepherd, 1989), post-entrapment hydrogen

diffusion (Hall and Bodnar, 1990; Ridley and Hagemann, 1996) or a primary methane-

dominated (possibly mantle) source.


75

Table 4.2 Mean, standard deviation and maximum concentrations of fluid inclusions from different vein types at New Celebration. Analyses are grouped as inclusion populations according to mineralization event, host rock, host vein inclusion type and salinity.

Concentrations are reported in parts per million (ppm). Salinity, XCO2, XCH4 and bulk density were obtained from microthermometric analyses. Standard deviations are reported to 1σ. Altn=alteration, Qz = quartz, cc=quartz-calcite, fsp=feldspar, aq=aqueous,

cb=carbonic.

Min. Stage

Host Rock

Vein Type

Sample No

Inclusion Type

Salinity wt.% NaCl equiv.

XCO2 (mole

%)

XCH4 (mole

%) Bulk Density (g/cm3) Na K Mg Ca Cu Pb Zn Sr Au Ag As Sb Bi Sn W Mo Ba U Th Cs Mn Fe K/Ca

1 M1 porphyry 2 1213279 Aq-cb 3.05

10 ± 1 to 33 ± 13

0 to 30 ±

1 0.78 ± 0.04 to 0.94 ± 0.01 11988

mean 1582 1147 2812 163 3 75 5 5 3 43 20 7 20 5 6 18 4 1 1 28 230 0.56 sd 809 660 1564 105 1 50 3 9 2 29 13 5 11 4 4 14 2 1 1 11 133

max 3240 2284 5110 350 6 173 12 52 9 108 45 16 42 12 13 70 10 3 3 43 422

2 M2 qz-

fsp porphyry

Qz-cc

altn

HBW-1250-

12-018 Aq-cb 4.51

48 ± 17 to 53 ± 28

0 to 1 0.65 ± 0.06 to 0.90 ± 0.05 17742 mean 3638 3704 574 66 30 106 56 6

1 118 31 30 20 309 6 55 3 3 2 39 584

6.34 sd 1745 519 384 53 13 87 57 10 149 27 29 14 197 5 44 2 2 2 28 384 max 6447 4172 1434 147 47 237 137 33 1 224 83 76 44 656 12 120 6 6 6 77 1204

3

133541 Aq-cb 5.12

16 ± 3 to 26 ±

8

0 to1 0.74 ± 0.11 to 0.95 ± 0.01 20142 mean 5406 2046 628 224 137 179 11 5 7 202 66 72 23 4 12 44 0 1 2 108 37

8.61 sd 3421 2436 448 133 88 149 6 7 6 156 82 68 14 4 9 36 0 1 1 36 max 11318 5926 1073 453 299 429 23 17 17 406 319 149 42 9 20 100 0 2 3 108 77

1213359 Aq-cb 3.8 17 ± 11 0 0.95 ± 0.03 14949

mean 5284 1061 5 25 16 22 3 1 1 3 1 5 457 4.98 sd 2328 671 6 12 16 9 2 1 1 1 1 2 181

max 2147 17 41 44 36 6 2 2 5 2 9 682

1213359 Aq (low salinity) 8.36 23888

mean 7098 1091 152 106 197 54 13 260 31 sd 2610 662 75 78 122 33 3 187 14

max 11570 1908 265 258 389 89 16 537 49

Post Au

M2 qz-fsp

porphyry

Qz-cc

altn

HBW-1250-

12-018

Aq (high salinity) 21

63998 mean 15127 2549 363 165

9 30 31 419

sd 13867 1655 390 138 21 26 406 max 29027 4440 805 323 9 53 48 869

3 133541 Aq (high salinity) 20.6 1.12 ± 0.02 to 1.16 ± 0.01 47714

mean 30990 420 5202 169 19 49 5 2 86 8 10 47 4 14 6 1 65 162 5.96

sd 4890 147 1299 74 10 37 2 2 44 3 15 33 2 7 2 1 51 57 max 45683 639 7163 360 37 87 8 3 144 11 39 93 6 24 7 3 147 233


76

There are few published data of metal concentrations in hydrothermal fluids

from orogenic lode gold deposits, and the majority of those published present bulk

crush-leach analytical techniques. Diamond (1990) and Yardley (1993) examined the

fluid characteristics of metamorphic gold-quartz veins from Brusson, in NW Italy and

Pike (1993) studied low-salinity gas-rich fluids in pegmatites from the Muiane deposit,

Mozambique. More recently Olivo et al. (2006) employed single inclusion laser

ablation-time of flight-inductively coupled plasma-mass spectrometry (LA-TOF-

ICPMS), in conjunction with crush-leach and microthermometry, to evaluate the fluid

compositions in barren and gold-bearing veins from the Sigma deposit in Canada. None

of these studies presented gold data. Relative to aqueous-carbonic fluids from Muiane

or Brusson, K, Mg, Cu, Mn and Fe concentrations in gold-related aqueous carbonic

fluid inclusions at New Celebration are elevated, whereas Na concentrations are lower.

Minor element/Na ratios of New Celebration fluids are generally an order of magnitude

lower than those from the Sigma deposit, with the exception of As, which is higher at

New Celebration. Major element/Na ratios (Mg, K, Ca), however, are up to an order of

magnitude higher in the New Celebration fluids.

More single inclusion data are available from porphyry systems (e.g. Audetat et

al., 1998; Audetat et al., 2000; Ulrich and Gunther, 2002; Klemm et al., 2007; Audetat

et al., 2008; Pudack et al., 2009), generally because sodium is used as the internal

standard for calculating absolute element concentrations (Allan et al., 2005) and fluid

salinities are higher in porphyry systems, although there is still a significant dearth of in

situ Au analyses. Low-salinity fluids from the Butte porphyry system (Rusk et al.,

2004), contain Na, K, Pb, Zn and Mn in similar concentrations to gold-related fluids

from New Celebration. Ulrich et al. (1999) publish Au concentrations averaging up to

10 ppm in vapor inclusions from the Grasberg porphyry Cu-Mo-Au deposit, and

Williams-Jones and Heinrich (2005) reported concentrations up to 57 ppm Au,

however, these Au concentrations were analyzed from high-salinity inclusions. Pudack

et al. (2009) reported Au concentrations up to 13 ppm in low-salinity aqueous-carbonic

fluid inclusion assemblages from deep porphyry and transitional zones at the Nevados

de Famantina porphyry Cu-Mo-Au system in Argentina.

The post-gold hydrothermal fluids at New Celebration are low temperature, high

salinity fluids with a characteristic Na, K , Mg and Ca signature. When comparing these

fluids with data sets from Canadian shield brines, sedimentary basin fluids,

metamorphic fluids, and geothermal fluids (Yardley, 2005 and references therein), it is


77

evident that the shield brines and basin fluids show no similarities to the New

Celebration post-gold fluids. The metamorphic, geothermal and magmatic fluids,

however, exhibit a number of similarities; Na, K and Mg concentrations are comparable

in all fluid types, whereas Ca and Cu concentrations in the New Celebration fluids are

most similar to magmatic fluids. Lead and Zn concentrations are more closely aligned

with metamorphic or geothermal fluids (Yardley, 2005 and references therein).

CHAPTER FIVE: SULFUR ISOTOPIC COMPOSITION AND MINERAL CHEMISTRY

78

5 CHAPTER FIVE: SULFUR ISOTOPIC COMPOSITION AND MINERAL CHEMISTRY OF SULFIDES, OXIDES AND GOLD

The isotopic and trace element composition of ore-stage sulfides can provide

valuable clues to potential fluid sources and the processes by which ore deposits form.

Pyrite grains associated with both mineralization stages were analyzed to determine

their sulfur isotope and trace element composition. Metamorphic and primary magnetite

grains in host rocks were analyzed to ascertain possible trace element contributions to

ore-stage sulfides.

5.1 Sulfur Isotopic Composition of Pyrite

5.1.1 Sample Selection and Analytical Procedure

The δ34S isotopic composition of pyrite from fifteen samples representing Stage

I and Stage II gold mineralizing events and four mineralization styles were analyzed by

either Nd-YAG laser ablation of in situ sulfides (Huston et al., 1995a) or conventional

techniques for pyrite separates (Robinson and Kusakabe, 1975) at the Central Science

Laboratory (CSL), at the University of Tasmania. Thirty in situ analyses and nine

conventional analyses were collected for this study. The conventional analyses

represented an initial reconnaissance study to evaluate the potential for a detailed in situ

analysis of ore-related sulfide. All results are reported in parts per thousand (per mil, ‰)

relative to the Canyon Diablo Troilite (CDT). Precision of the standards is typically

±0.1 per mil CDT for in situ analyses and ±0.3 per mil CDT for homogeneous mineral

separates. Pyrite grains were typically too small to investigate the possibility of isotopic

zonation therefore all in situ analyses were taken from the sulfide grain centers.

In situ samples were prepared as double-polished thick sections either at the

University of Tasmania or by Pontifex Associates in Adelaide. Samples were mounted

onto a glass slide with super-glue then polished to a thickness of approximately 200 µm.

Prior to analysis, the samples were soaked off the slides with acetone and ultrasonically

cleaned sequentially in warm soapy water, distilled water and acetone, then oven dried

at approximately 80 °C. Samples were then mounted on a glass pedestal and placed into

the sample chamber, which was evacuated to a vacuum better than 10-2 torr. Sulfide

grains were ablated in an oxygen atmosphere for 2 seconds by an 18 watt Quantronix


79

model 117 Nd:YAG laser. Ablation produces a small amount of SO2, which is removed

from the oxygen atmosphere prior to analysis by circulating the SO2/O2 mixture through

a liquid nitrogen trap, where SO2 condenses and O2 is pumped away. Carbon dioxide,

produced by carbonate-bearing samples, was removed by cold-finger separation through

an N-Pentane trap. The purified SO2 gas was analyzed by a VG Sira Series II mass

spectrometer.

A laboratory-dependent correction factor and a fractionation factor were applied

to the raw 34S data into 34SCDT values. Standards from Rosebery and Broken Hill were

run daily prior to sample analysis in order to determine the laboratory dependent

correction factor. Fractionation factors for pyrite and pyrrhotite are 4.75 per mil and

4.12 per mil respectively.

For conventional analyses, sulfide mineral separates (8-25 milligrams,

depending on sulfide species, purity and anticipated SO2 yield) were ground with 150

milligrams of cuprous oxide in an agate mortar, placed in a pre-ignited mullite ceramic

boat and ignited in vacuo (Robinson and Kusakabe, 1975). The use of excess Cu2O in

this method ensured the low pO2 favorable for SO2 production, and that negligible SO3

was produced. All gases from the combustion were condensed into a Pyrex glass trap

held under liquid nitrogen. Contaminant H2O was frozen out at the freezing point of

acetone (-95 °C), and CO2 was removed from the condensed SO2 at the freezing point

of n-pentane (-131 °C). Purified SO2 was collected into a Pyrex glass gas bottle under

liquid nitrogen and then connected to the sample inlet of the mass spectrometer for

isotope ratio analysis. Isotopic analysis of the extracted SO2 was performed with a VG

SIRA 10, Series 2 triple-collector mass spectrometer, using reference gas SO2 calibrated

against NBS 123 sphalerite, IAEA-S-1, Broken Hill galena and Rosebery galena as

working standards to establish a calibration curve.

5.1.2 Results

The majority of both Stage I and Stage II gold-related pyrites at New

Celebration had negative δ34S values (Table 5.1, Fig. 5.1), although the range of values

both within and between mineralization styles varied widely. Results of laser ablation

analyses of Stage I gold related samples ranged from -7.6 to +3.8 per mil (mean -2.6 ‰;

n=18) whereas Stage II gold related samples ranged from -10.6 to -3.2 per mil (mean -

7.1 ‰; n=21). The data define three discrete populations (Fig. 5.1) with little overlap


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Figure 5.1 Total range of δ34S values from ore-related pyrite from all mineralization styles at New

Celebration (this study, Hodkiewicz, 2003) and potential sulfur sources. Blue bars = Stage I

mineralization; red bars = Stage II mineralization. Vertical dashes = mean. The gray shaded area

corresponds to average δ34S values of pyrite from other Yilgarn gold deposits (summarized by

Hodkiewicz, 2003). Values for I-type granite from Ohmoto (1986), Yilgarn crust from Lambert et al.

(1984) and Archean seawater from Ohmoto and Goldhaber (1997).

Table 5.1 Sulfur isotopic composition of pyrites from New Celebration Stage I and Stage II gold

mineralization samples as determined by laser ablation ICP-MS analysis. Samples with an asterisk (*) are

from Hodkiewicz (2003)

Sample No Min. Event

Min. Style Sample Description Pyrite Description Method δ34S (‰) Precision

1213279 Stage I Porphyry M1 carbonate altered plagioclase porphyry

Anhedral, grains intergrown, 1000μm

LA -4.14 0.006


Anhedral, several grains in foliation plane, 300μm

LA -5.72 0.005


Anhedral, elongate, located in foliation plane, 500μm

LA -6.26 0.018


Euhedral, disseminated, 300μm

LA -3.15 0.010


Anhedral, disseminated, 250μm

LA -7.36 0.020



LA -6.06 0.003


Subhedral-euhedral, disseminated, 100-200μm

LA -7.49 0.004


Fine-grained, anhedral, located in S3NC foliation planes

LA -6.90 0.008

1213226 Stage I Mylonite Quartz-carbonate mylonite Anhedral, sheared, located in S3NC foliation planes, 400μm

LA 3.77 0.220

1213226 Stage I Mylonite Quartz-carbonate mylonite Anhedral, aligned along S3NC foliation planes, 200μm

LA 0.57 0.011


81




LA 1.50 0.003


LA 2.19 0.019


LA 2.34 0.017


LA 0.58 0.009

133555 Stage II Contact Quartz-carbonate-fuchsite-altered contact between M2 quartz-feldspar porphyry and high-Mg basalt

Semi-massive, anhedral grains, aligned along S3NC foliation planes at contact, 400-1000μm

LA -7.19 0.005



LA -8.28 0.013



LA -6.08 0.005



LA -7.26 0.011



LA -6.72 0.014



LA -8.34 0.006

1250_12-018 Stage II Contact Quartz-carbonate-fuchsite-altered contact between M2 quartz-feldspar porphyry and high-Mg basalt


LA -3.22 0.005


82





LA -3.28 0.017



LA -4.71 0.011



LA -3.89 0.007

1213359 Stage II Fracture M2 albite-carbonate altered quartz-feldspar phyric porphyry

Anhedral, 200-500μm LA -10.61 0.031


Anhedral, 200-500μm LA -10.26 0.034


Anhedral, 200-500μm LA -9.39 0.010


Anhedral, 200-500μm LA -7.40 0.023


Anhedral, 200-500μm LA -8.55 0.007


Anhedral, 200-500μm LA -7.62 0.019

121763* Sericite-altered sheared porphyritic intrusion

Subhedral, 100μm LA -1.41 0.12

121766* Biotite-dolomite-chlorite-altered ultramafic schist

Subhedral, 100μm LA 3.92 0.015

121776* Chlorite-calcite-albite-altered mafic schist

Euhedral, 300μm LA 5.54 0.038

121784* Albite-hematite-altered sheared felsic porphyry

Euhedral, 800μm LA -8.64 0.032




Subhedral, 500μm LA -6.04 0.012

121788* K-feldspar-albite-ankerite-altered tholeiitic mafic schist


121788* K-feldspar-albite-ankerite-altered tholeiitic mafic schist

Euhedral, 1000μm LA -5.49 0.016


83

between populations and may provide indications to potential sulfur sources and

processes.

5.1.3 Interpretation of Results

The sulfide sulfur isotopic values collected during this study contrast with the

predominantly positive δ34S values (0-5 ‰) reported by Golding et al. (1990c),

Hodkiewicz (2003 and references therein) and Hodkiewicz et al. (2009), for ore-related

pyrites from most gold deposits in the Eastern Goldfields (with the exception of the

Porphyry, Golden Mile and Victory-Defiance deposits) and 0-9 per mil for ore-related

sulfides in Archean orogenic lode gold deposits worldwide (with the exception of

Hemlo, Lakeshore/Macassa, Canadian Arrow and Kelore, which have much larger δ34S

ranges) reported by Colvine et al. (1988) but are consistent with previous analyses of

ore-stage pyrite from New Celebration undertaken by Hodkiewicz (2003) and

Hodkiewicz et al. (2009).

The hydrothermal fluids that precipitated gold-stage pyrite at New Celebration

were significantly more oxidized than the average Archean lode gold deposit (cf.

McCuaig and Kerrich, 1998). Either they were intrinsically oxidized from their source

or they were oxidized during gold precipitation by: (1) in situ fluid oxidation due to

reaction with iron-rich wall rocks (Couture and Pilote, 1993), (2) fluid mixing (Uemoto

et al., 2002) or (3) fluid oxidation during phase separation (Drummond and Ohmoto,

1985).

5.1.3.1 Sulfur Sources

Potential sulfur sources for Archean lode-gold ore fluids in the Yilgarn include:

1) sulfides in the host greenstone sequences; 2) dissolved seawater sulfur (in deposits

where there is potential for significant seawater water infiltration); 3) sulfur-bearing

magmatic volatiles, or 4) fluids that have equilibrated with magmatic sulfides (Kerrich,

1986). Sulfides in mafic, ultramafic and sedimentary rocks of the Yilgarn Craton have

δ34S values between +1 and +5 per mil (Donnelly et al., 1978; Seccombe et al., 1981;

Lambert et al., 1984), and Archean seawater sulfate likely had values ranging between

+2 and +10 per mil (Ohmoto and Goldhaber, 1997) (Fig. 5.1). There are no available

data on the sulfur isotopic composition of Yilgarn granites; however, Witt and Swager

(1989) described most southeastern Yilgarn granitoids as being either biotite

monzogranite or monzogranite with I-type affinities. I-type granites worldwide have


84

δ34S values between -5 and +7 per mil (Ohmoto, 1986). Significant overlap in these data

sets means that sulfur isotopes are not by themselves diagnostic of a source. They may

provide, however, some information about processes.

5.1.3.2 Ore Forming Processes and their Influence on the Sulfur Isotopic Composition of Pyrite

Gold mineralization occurs in response to changing chemical conditions of the

ore fluid, typically the fluid redox state or pH, which takes place due to physical

changes to the ore fluid, such as fluid immiscibility, fluid mixing or interaction with

reactive wall rocks (Seward, 1973, 1984; Mikucki and Groves, 1990; Mikucki, 1998).

Most researchers agree that gold in orogenic lode gold systems is transported as a

sulfide complex (Phillips and Groves, 1983; Mikucki, 1998; Loucks and Mavrogenes,

1999), and as such, the sulfur isotopic composition of sulfides precipitated from gold-

bearing hydrothermal fluids reflects the sulfur source and/or the in situ physic-chemical

conditions during mineralization, such as temperature, pressure, pH and the oxidations

state of the host rocks (Ohmoto and Rye, 1979; Ohmoto and Goldhaber, 1997).

According to Lambert et al. (1984), Phillips et al. (1986) and Golding et al. (1990c) an

increase in the redox state of the fluid lowers gold solubility significantly, thereby

creating conditions that favor gold precipitation (Fig. 5.2).

Interaction between the ore fluids and iron-rich wall rocks likely facilitated

much of the gold mineralization at New Celebration. In all mineralization styles pyrite

hosts gold, and gold enrichment shows a close correlation with increasing pyrite

(Williams, 1994; Nichols, 2003). Additionally, gold is located predominantly within the

iron-rich wall rock in all mineralization styles except Fracture-style, where narrow

sericite-filled cracks contain the gold-bearing pyrite. Extensive ankerite alteration

accompanies all gold mineralization styles, and pyrite replaces magnetite with

increasing proximity to mineralization. The unaltered intermediate and felsic porphyry

host rocks likely did not provide enough iron to facilitate wall rock reactions, however,

extensive pre-mineralization magnetite and hematite alteration (Nichols, 2003) resulted

in a significant increase in the amount of modal iron which would facilitate fluid-rock

desulfidation according to the following reactions:.

Fe2O3 + 4H2S0 = 2FeS2(py) + 3H2O + H2 (1)

or

(Fe2+2Fe3+)O4 + 6H2S = 3FeS2 + 4H2O + 2H2 (2)


85

which could cause gold precipitation according to the following reaction

Au(H2S)2- + H+ + 1/2H2(g) = Au + 2H2S0 (3)

Palin and Xu (2000), however, indicated that this reaction would not effect a change to

the oxidation state of the dissolved sulfur species, therefore there would be no shift to

the isotopic composition of pyrite. An alternative reaction that causes gold to precipitate

in the wall rocks is the carbonation of magnetite to form iron-bearing carbonates

(Phillips et al., 1996). This results in significant fluid oxidation via the following

reactions:

(Fe2+2Fe3+)O4 + 3CO2 = 3Fe2+CO3 + 0.5O2 (4)

and

H2S + 2O2 = SO42- + 2H+ (5)

These reactions destabilize the reduced gold bisulfide complexes and promote gold

precipitation by the following reaction

2(Fe2+2Fe3+)O4 + 6HAu(HS)2 + 0.5O2 = 6Au + 6Fe2+S2 + 9H2O (6)


86

Figure 5.2 Plot of oxygen fugacity (log fO2) vs. pH showing gold solubility contours (0.01, 0.1, 1.0 and

10.0 ppm) for gold–bisulfide complexes (Hodkiewicz et al., 2009). Oxidation of fluid to higher ƒO2 is

the most efficient method of removing gold from solution.

Lambert et al. (1984) and Phillips et al. (1986; 1996) suggested that the

extensive carbonate alteration halo around the Golden Mile deposit indicated that

reduced ore fluids became oxidized by magnetite carbonation adjacent to the gold lodes.

Palin and Xu (2000) and Couture and Pilote (1993) also suggested the same mechanism

for gold precipitation and accompanying fluid oxidation at Victory (Western Australia)

and Francoeur 3 (Quebec), respectively. Hodkiewicz (2003) determined a broad

negative correlation (r2=0.73, n=5) between gold grade and sulfide sulfur isotopic

composition at New Celebration and interpreted this as evidence for in situ ore fluid

oxidation and gold precipitation by carbonate alteration of host rock magnetite,

however, this interpretation was based on a very small, statistically meaningless sample

population. In contrast, this study found no correlation between sulfide sulfur isotopic

composition and gold grade (r2=0.10, n=28). Further, Mikucki (2000, 2001, unpublished

AMIRA reports), using quantitative reaction flow modeling of reduced lode gold fluids

with a number of greenstone sequence host rocks, showed that this model for in situ

fluid oxidation was not viable at high fluid-rock ratios except where CO2-CH4 exchange

is chemically inhibited. As neither precipitation mechanism would facilitate in situ


87

oxidation of the ore fluid, the sulfur isotopic composition of Stage I and Stage II

Contact-style ore-stage pyrite may likely reflect the composition of the ore fluids.

Fluid inclusion petrography suggests intermittent phase immiscibility during

Stage II gold mineralization. During phase separation reduced gases (H2S, CH4 and H2)

are preferentially partitioned into the gas phase, thus the liquid becomes more oxidizing.

As a result, some of the remaining reduced species in the liquid, such as H2S, will be

oxidized to HSO4-, which is enriched in 34S. Consequently, the reduced sulfur left

behind is depleted in 34S, therefore sulfides that precipitate from the residual liquid

phase are also 34S depleted (Drummond and Ohmoto, 1985). Phase separation is

consistent with the observations made from type 3 quartz veins and quartz and

carbonate alteration related to Stage II gold mineralization and accounts for both the

negative sulfur isotopic composition and the spread in δ34S ratios observed in Stage II

ore-related pyrites. Hodkiewicz et al. (2009), in their detailed study of the Victory

deposit in Kambalda, indicated that fault-induced phase separation, particularly in

shallowly-dipping dilational structures, and back-mixing of modified fluids would lead

to negative sulfide sulfur isotopic compositions and wide spreads in observed values.

They postulated that host structures exerted the greatest control over the isotopic

composition of ore-hosting sulfides and discounted the need for intrinsically oxidized

ore fluids. Depleted sulfur isotopic signatures may also result from fluid mixing (cf.

Neumayr et al., 2008), either by the addition of an oxidized CO2-dominated fluid to

reduced aqueous-carbonic inclusions, or by the addition of CH4 to the ore fluids, which

would drive the solvus towards higher temperatures and pressures and increase the two-

phase field in the H2O-CO2 system (McCuaig and Kerrich, 1998) (see section 4.4.5.2,

Chapter 4).

Light sulfur may also be contributed by pyritic black shales, such as the Kapai

slate, a prominent marker horizon in the Kalgoorlie-Kambalda terrane (Swager, 1989;

Swager et al., 1995). Kapai slate is, however, volumetrically insignificant in the New

Celebration area and immediate surrounds (Langsford, 1989).

5.1.4 Summary

The stable isotopic compositions of sulfides from New Celebration define three

populations: pyrites from Stage I Mylonite-style, which have the least depleted isotopic

signature, sulfides from Stage I Porphyry-style and Stage II Contact-style, which show

considerable overlap in values and range, and pyrites from Stage II Fracture-style,


88

which display the most depleted signature. A strong positive correlation between gold

grade and pyrite abundance (Williams, 1994; Nichols, 2003) in all mineralization styles

except Fracture-style, which indicates that wall rock reaction was the mechanism by

which gold precipitated, and evidence for fluid immiscibility and fluid mixing in Stage

II mineralization, suggests that the variability in sulfide sulfur isotopic composition

observed in the different mineralization styles reflects the different ore-forming

processes and/or fluid sources. As wall rock reactions, either by magnetite sulfidation or

carbonation, do not facilitate in situ fluid oxidation, the sulfur isotopic composition of

sulfides associated with Stage I mineralization, likely represents the composition of the

sulfur, and by association, the fluid source. The fluid source is at present unconstrained,

however, the most likely sources are from devolatilized metamorphic crust or felsic

magmatic crust. Contributions from carbonaceous shale units postulated by other

authors to be potential sources of C, S and Au for orogenic deposits (e.g. Junction;Polito

et al., 2001; Golden Mile (Oroya lodes) Bateman and Hagemann, 2004; Carlin, Sukhoi

LogLarge et al., 2009) are considered unlikely at New Celebration given the

volumetrically insignificant amounts of carbonaceous units in the vicinity.

The sulfide sulfur isotopic composition of Stage II mineralization, for which

there is evidence of fluid mixing between oxidized CO2-rich fluids and mixed aqueous-

carbonic fluids, and evidence for at least local phase immiscibility, likely reflects an

interplay between the source of the hydrothermal fluids and in situ oxidation of the ore

fluids during gold mineralization. Evidence for CO2-rich fluids in the fluid inclusion

record suggest a possible magmatic contribution to the hydrothermal fluid system.

5.1.5 Comparisons with other Hydrothermal Mineral Systems

5.1.5.1 Orogenic Lode Gold Deposits

McCuaig and Kerrich (1998) considered that the majority of 34S(sulfide, sulfate)

values from Archean orogenic lode gold deposits around the world ranged between 0

and +9 per mil. They interpreted these values to indicate that ore fluid redox states were

below the SO2/H2S boundary and that sulfur was derived from a uniform source with a

34S composition between -1 and +8 per mil. Potential sulfur sources include dissolved

sulfur in seawater, sulfur-rich magmatic gases or sulfides within the host succession

(Kerrich, 1986), all of which have published sulfur isotopic compositions between 0 and

+10 per mil (Donnelly et al., 1978; Seccombe et al., 1981; Lambert et al., 1984; Ohmoto

and Goldhaber, 1997). Sulfur isotopic ratios are more varied in deposits hosted within


89

Proterozoic rocks (Partington and Williams, 2000) and cluster around 0 per mil in

Phanerozoic deposits (Bierlein and Crowe, 2000). There are, however, a number of

studies on deposits with sulfide sulfur isotopic signatures that vary significantly from

mean values (down to -27‰), and whose isotopic compositions possibly reflect the

input from alternative sulfur sources or in situ modification by various ore-forming

processes. Australian examples include the giant Golden Mile deposit (Phillips et al.,

1986; Hagemann et al., 1999), the small (11 t Au), monzonite-hosted Porphyry deposit

(Hodkiewicz, 2003; Hodkiewicz et al., 2009) and the Victory-Defiance deposit in

Kambalda (Palin and Xu, 2000; Hodkiewicz, 2003; Hodkiewicz et al., 2009).

International examples include Hemlo (Thode et al., 1991), Canadian Arrow and

Lakeshore/Macassa (Cameron and Hattori, 1987), gold-related sulfides of the Ashanti

belt (Oberthuer et al., 1996), the Alaska range (Goldfarb et al., 1991) and Donlin Creek

(Goldfarb et al., 2004).

5.1.5.1.1 Eastern Goldfields Province

The sulfur isotopic values of ore-related pyrites from orogenic lode gold

deposits of the Eastern Goldfields Province range between -10.2 and + 12.7 per mil,

with average mean values between -4.0 and +4.0 per mil (Hodkiewicz et al., 2009 and

references therein). Sulfides from most deposits have positive mean values and narrow

ranges (Hodkiewicz et al., 2009), however, some deposits, such as New Celebration

(Hodkiewicz, 2003; Hodkiewicz et al., 2009; Hodge et al., in revision), Porphyry

(Hodkiewicz, 2003; Hodkiewicz et al., 2009), Golden Mile (Phillips et al., 1986;

Hagemann et al., 1999), and to a lesser extent, Victory-Defiance (Hagemann and

Cassidy, 2000; Palin and Xu, 2000; Hodkiewicz, 2003; Hodkiewicz et al., 2009), have

negative mean values and broad ranges. At New Celebration, Porphyry, and Victory,

Hodkiewicz et al. (2009) established a negative correlation between gold grade and

sulfide sulfur isotopic composition, suggesting that pyrites with more depleted values

correlated with higher gold grades, however this correlation was not borne out at New

Celebration by this study. At New Celebration, Hodkiewicz et al. (2009) concluded that

the depleted isotopic composition of ore-stage pyrite resulted from carbonation of wall

rock iron oxides by CO2-bearing hydrothermal fluids. This interpretation does not stand

up to rigorous examination as, firstly, the most depleted values are reported from

sulfides hosted within M2 feldspar-phyric porphyries, which do not contain Fe-oxide

minerals, and secondly, in situ fluid oxidation by carbonate alteration of wall rock

magnetite is not viable in environments with high fluid-rock ratios (Mikucki, 2000;


90

2001), such as those expected in a large fault system like the BLFZ. Generally,

however, Hodkiewicz et al. (2009) concluded that the isotopic composition of ore

related pyrites around the Yilgarn resulted from fluid oxidation due to faulting-induced

phase separation in gently dipping dilational structures and back-mixing of modified ore

fluids. They concluded that this process would lead to negative 34S(py) values and

extreme ranges of values without invoking the need for an intrinsically oxidized ore

fluid, such as that derived from magmatic sources, or any meteoric water contributions.

At the Golden Mile, Bateman and Hagemann (2004) concluded that the depleted values

(<-10 ‰) and extreme range (22 ‰ from Fimiston-style mineralization) in 34S values

recorded in sulfides from Fimiston and Oroya lodes resulted from a combination of

sulfur sources (igneous, sedimentary and seawater) and multiple mineralization

processes, such as phase separation and fluid mixing. In contrast, Phillips et al. (1986)

considered that the depleted sulfur isotopic composition of Golden Mile pyrites resulted

from locally oxidizing environments induced by wall rock reactions within ductile shear

zones in differentiated host rocks. Evans et al. (2006), using HCh fluid modeling,

demonstrated that the negative 34S(pyrite) values at Golden Mile could have been

generated by reactions between an Fe3+-bearing mafic wall rock and a sulfur-CO2-Au-

bearing ore fluid, without the need for an external oxidized fluid source.

5.1.5.1.2 Global Examples

As with Eastern Goldfields Province, there are a number of deposits worldwide,

and particularly in North America, which contain sulfides that are systematically

depleted in 34S. An example is the Hemlo deposit, where Thode et al. (1991) concluded

that the wide range of values (-15.9 to +1.0 ‰) observed in ore-stage pyrites resulted

from fluid rock reactions and isotopic exchange between pyrite and sedimentary barite.

Other examples include Canadian Arrow (34S= -12 to -10 ‰ ) and Lakeshore/Macassa

(34S= -14.4 to -9.1 ‰), the isotopic compositions of which Cameron and Hattori

(1987) attributed to a magmatic fluid source. Oberthuer et al. (1996) reported negative

compositions (-10.2 to -5.3 ‰) from gold-related sulfides from the Ashanti belt in

Ghana, and attributed these values to result from pyrite formation from metamorphic

fluids that had equilibrated with the host sedimentary sequence. The 34S values from

gold-related sulfides from the Eocene Juneau belt deposits of Alaska range between -

17.8 and +1.2 per mil and are among the most depleted of orogenic lode gold deposits

worldwide. Goldfarb et al. (1991) considered that the ore forming fluid was

unequivocally of metamorphic derivation with an inferred regional 34S estimate of -7


91

to -5 per mil. They attributed the highly variable sulfide sulfur isotopic values to reflect

the composition of additional sulfur derived locally, within and immediately adjacent to

the host rocks, with the most depleted values reflecting a black phyllite host and the

most enriched values reflecting relatively oxidized igneous host rocks. The late

Cretaceous Donlin Creek deposit in southwestern Alaska also contains gold-related

sulfides with very depleted values, ranging between -27.2 and -7.3 per mil (Goldfarb et

al., 2004). Goldfarb et al. (2004) considered that these values reflected the values of

diagenetic pyrite from the host flysch basin and that the ore fluid was derived from

either regional-scale metamorphic devolatilization of the basin above rising mantle

melts or from intrusions with a significant flysch component.

5.1.5.2 Other Gold Mineral Systems

The 34S composition of ore stage sulfides (pyrite, marcasite, arsenopyrite) in

Carlin-type gold deposits ranges between 0.0 and 17.0 per mil, which at 200 °C

indicates an ore fluid composition between -1.0 and +19.0 per mil (Hofstra and Cline,

2000). Hofstra and Cline (2000) noted that this range was similar to diagenetic pyrite

and organic sulfur in lower Paleozoic sedimentary rocks of the Carlin trend and

interpreted this to indicate that at least some of the sulfur was derived from dissolved

pyrite or the metamorphic desulfidation of pyrite. They also concluded that the heaviest

34S values likely resulted from sulfur derived from barite or anhydrite, whereas the

lightest values may have resulted from sulfur derivation from magmatic fluids. In high

sulfidation epithermal deposits, light isotopic compositions of ore-stage sulfides ranging

between -10 and -1 per mil and are generally interpreted to indicate magmatic ore fluids

(Cooke and Simmons, 2000). Light sulfur isotopic signatures generally characterize

alkaline-hosted epithermal and porphyry deposits (Ahmad et al., 1987a; Richards and

Kerrich, 1993; Thompson, 1998), which possibly indicate sulfur contributions from

alkaline magmatic systems, or represent progressive oxidation of the ore fluids by

processes such as phase separation (Richards and Kerrich, 1993). The isotopic

composition of ore-related sulfides in intrusion-related deposits generally ranges

between -5.0 and +5.0 per mil (Thompson and Newberry, 2000, and references therein),

which is typically interpreted to represent contributions from magmatic sulfur. Some

deposits, however, have sulfides with significantly lighter values, e.g., Donlin Creek, (-

22 to -12 per mil, Szumigala et al., 2000) and Scheelite Dome (Mair et al., 2006, -15 to -

10 per mil), which in both cases were interpreted to reflect sulfur derived from adjacent

metasedimentary country rocks.


92

5.2 Sulfide, Oxide and Gold Mineral Chemistry

5.2.1 Sample Selection, Preparation and Analytical Procedure

Eleven samples representing Stage I and Stage II ore-related pyrites, and

metamorphic and hydrothermal magnetites and ilmenites were analyzed by laser

ablation inductively coupled plasma mass spectrometry (LA-ICP-MS). The samples

were collected from diamond drill core from within the Hampton-Boulder and Jubilee

open pit and underground deposits. The purpose of these analyses was to chemically

fingerprint oxides, sulfides and gold from different host rocks, mineralization stages and

mineralizing events, and to compare trace element compositions of hydrothermal fluids

(as determined by LA-ICP-MS of individual fluid inclusions) with ore-stage pyrite and

gold grains to evaluate potential metal sources and constrain ore-forming processes.

Analyses were conducted at the ARC Centre of Excellence in Ore Deposits in Hobart

under the supervision of Leonid Danyushevsky and Sarah Gilbert.

Samples were mounted into a one-inch diameter epoxy block and polished with

aluminum oxide powder. The samples were then photographed, to identify suitable

sulfide and oxide grains, and circled with a fine tipped marker to enable easier location

of the grains once in the sample chamber. Grains were ablated in a high-purity He

atmosphere by a New Wave UP-213 Nd:YAG Q-switched Laser Ablation System.

MEOLaser 213 software controlled all laser parameters including spot-size, laser

energy, pulse rate, and laser firing. A 40 µm diameter beam at 40Hz and 60% power

ablated most grains, although smaller grains required a smaller diameter beam. A

mixture of He and Ar carried the ablated material to the Agilent HP4500 Quadrapole

ICP-MS. Each spot analysis took 90 seconds, including an initial 30 seconds during

which no ablated material was analyzed in order to establish background counts. The

ICP-MS was tuned daily using NIST-612 glass, and an in-house standard (STDGL2b-2)

was run every 90 minutes to calculate concentrations of unknowns and to correct for

instrument drift. Selected integration intervals were then converted from counts per

second to concentration using stoichiometric iron (for sulfides and oxides) and gold as

an internal standard (Appendix 7).

Pyrite, magnetite, ilmenite and gold were analyzed for Ti, Cr, Mn, Fe, Co, Ni,

Cu, Zn, As, Se, Zr, Mo, Ag, Cd, Sn, Sb, Te, Ba, La, W, Au, Tl, Pb, Bi, Th, and U. For

ease of comparison on extended multi-element diagrams, concentrations were

normalized to average lithospheric abundances (Clarke values) using the values of


93

Taylor (1964) and Vinogradov (1964, all elements except Te), taken from Rosler and

Lange (1972, p.230-231).

5.2.2 Results

Trace elements are hosted in pyrite either as mineral inclusions (e.g. Cu, Pb, Zn,

Ba, Bi, Ag, Sb) or as non-stoichiometric (e.g. As, Tl, Au, Mo) or stoichiometric (e.g.

Co, Ni for Fe or Se, Te for S) lattice substitutions (Huston et al., 1995b). Metamorphic

and hydrothermal recrystallization will remove those elements incorporated either as

inclusions or non-stoichiometric substitutions, but the concentrations of those elements

incorporated in pyrite as stoichiometric substitutions are unaffected (Huston et al.,

1995b). In magnetite, the substitution of various elements (Ti, Al, Mn, Mg, Cr, Zn, Ga,

Ni) for Fe2+ or Fe3+, is dependent on temperature, oxygen fugacity, the availability of

elements in the melt or hydrothermal solution and the order of crystallization (in the

case of primary igneous magnetite (Hodge, 1997)). The location of trace elements

within the host minerals can be determined by comparing the analytical results with

petrographic observations and by observing peak widths on individual mineral spectra.

Elements which are elevated in pyrite, such as Ni and Co, and are analyzed at relatively

constant levels, (i.e. they have a very broad peak, Fig. 5.4), but are not incorporated in

Ni or Co sulfides, likely occur as stoichiometric substitutions within the pyrite or oxide

crystal lattice. In contrast, elements such as Te or Pb-Bi, which are typically analyzed at

erratic levels and form spikes on the mineral spectra, likely occur as mineral inclusions

(e.g., tellurides or galena, respectively) within the pyrite or oxide.

5.2.2.1 Pyrite

Mineral spectra of individual analyses illustrate a number of differences (and

similarities) between pyrites from the different ore stages and mineralization styles.

Pyrites from both mineralizing stages and all mineralization styles contained measurable

Ni and Co incorporated within the pyrite crystal lattice (Fig. 5.4). Nickel


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Figure 5.3 LA-ICP-MS spectrum of ubiquitous Ni and Co incorporated in a Stage I ore-stage pyrite as a

stoichiometric substitution within the pyrite lattice.

and Co are the most common elements found in pyrite (Loftus-Hills and Solomon,

1967) and exhibit complete isomorphous solid solution with Fe in pyrite at temperatures

below 400 °C (Moh, 1980). Stage I ore-stage pyrites also contained Ti, W, Pb, Zn, Cr,

Co, and As within the pyrite crystal structure. Titanium, Mn, Cr, Zn, Cu, W, Mo, Au,

Ag, As Te, Sb, Bi, U, Th, La, and Zr were commonly observed as inclusions in both

Stage I and Stage II pyrites, typically in specific combinations. Gold, Ag, Te and Pb

(Fig. 5.5) were observed together reflecting the presence of Au-Ag-Pb tellurides, which

is consistent with Nichols’ (2003) petrographic observations. Lead and Bi were

typically observed in tandem, reflecting galena and/or bismuthinite inclusions, also

consistent with petrographic observations. Zirconium, U, Th and La were observed

together, probably reflecting silicate inclusions such as zircon or thorite within the

sulfides.

5.2.2.2 Fe-oxides

Mineral spectra from metamorphic fine-grained magnetite in Stage I-related

mylonitized monzonite, pre-mineralization hydrothermal magnetite in high-Mg basalt,

and hydrothermal ilmenite in dolerite show a number of contrasts between the different

Fe-oxides. The hydrothermal magnetites and ilmenites were compositionally simple and


95

comprised Fe, Mn, Co, Cr, Ni, Ti, and Zn, and Ti, Mn, Fe, Co, Zn, Ni, and W,

respectively. In contrast, metamorphic magnetites comprised lattice-bound Fe, Ni,

Figure 5.4 LA-ICP-MS spectrum of gold-silver-lead telluride inclusion in a Stage II ore stage pyrite from

the New Celebration deposit.

and Co, but also contained Ti, Cr, Zn, As, Bi, and W in variable proportions within the

crystal lattice. The hydrothermal magnetites and ilmenites typically only contained

zircon inclusions, although rare grains also contained Pb-Ti, Sn, Ba, and Mo-bearing

inclusions, whereas metamorphic magnetite contained abundant poly-metallic (Pb, Ti,

Cr, Bi, Ba, Sb, W, Mn, Zn-bearing) and zircon inclusions.

5.2.2.3 Gold

Gold analyses revealed minor chemical differences between Stage I (Porphyry-

style, 3 grains analyzed) and Stage II (Contact- and Fracture-style, 1 grain and 4 grains

analyzed, respectively). Stage I gold contained only gold and silver within the lattice,

and contained rare Cu, Pb, Ba-Ti and Pb-Bi inclusions, whereas Stage II gold contained

trace amounts of Pb and Cu, in addition to Au and Ag, within the crystal lattice. Stage II

grains also hosted rare Pb-Bi (Fig. 5.6) and Ba-bearing inclusions. These likely

represent sulfide (galena and/or bismuthinite) and sulfate (barite) inclusions within the

gold grains, which is consistent with petrographic and scanning electron microscopy

(SEM) observations (Nichols, 2003) on these samples.


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Figure 5.5 LA-ICP-MS spectrum of a gold-silver grain with a gold-silver-lead-bismuth inclusion

5.2.3 Interpretation of Mineral Chemistry

Figure 5.7 illustrates the abundances of all the elements analyzed, except Fe,

relative to average crustal abundances (data from Rosler and Lange, 1972) in pyrites

from Stage I (Mylonite- and Porphyry-style) and Stage II (Contact- and Fracture-style)

mineralization, in addition to metamorphic magnetite from mylonitized monzonite and

hydrothermal Fe-oxides from high-Mg basalt and dolerite. It clearly illustrates that

pyrites from Stage II Fracture-style mineralization show markedly different trace

element patterns than those pyrites related to both Stage I mineralization styles and

Stage II Contact-style mineralization. They display significant depletion of Ni, Co, Mn,

Cr, and Zn but enrichment of Pb and Bi relative to Stage I and Stage II Contact-style

pyrites, which may reflect the influences of felsic versus mafic and intermediate host

rocks, ore forming processes, fluid sources or a combination of these factors (cf. Phillips

et al., 1988; Carew et al., 2006).

5.2.3.1 Tellurium

Using both standard microscopy and SEM, Nichols (2003) observed calaverite

(AuTe2), petzite (Ag3AuTe2), hessite (AgTe2), tetradymite (Bi2Te2S) melonite (NiTe2),

and altaite (PbTe) associated with Stage I gold mineralization, but did not report

tellurides from Stage II. It is notable that pyrites from both mineralizing stages


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Figure 5.6 Spider diagram illustrating the abundances of all the elements analyzed, except Fe, relative to

average crustal abundances (data from Rosler and Lange, 1972) in pyrites from Stage I (Mylonite- and

Porphyry-style) and Stage II (Contact- and Fracture-style) mineralization, in addition to metamorphic

magnetite from mylonitized monzonite and hydrothermal Fe-oxides from high-Mg basalt and dolerite,

illustrating that pyrites from Stage II Fracture-style mineralization show markedly different trace element

patterns than those pyrites related to both Stage I mineralization styles and Stage II Contact-style

mineralization. This likely reflects differing contributions from wall rocks and ore fluids for the different

mineralization styles and events.

and all mineralization styles contained Te inclusions, and that all mineralization styles

exhibit a positive correlation between Au and Te in pyrite (Fig. 5.8). Further, the highest

Te concentrations are observed predominantly in pyrite from Fracture and Contact

mineralization styles. Afifi (1988) indicated that the presence or absence of tellurides

with ore minerals such as pyrite, pyrrhotite, arsenopyrite, galena, sphalerite or

chalcopyrite, is a function of ƒTe2, which is controlled by the availability of Te at the

source and locally by buffering reactions between vein minerals and the hydrothermal

fluid. They concluded in their study of telluride paragenesis and geochemistry from 32

vein, skarn, massive sulfide and magmatic deposits from around the world, that telluride

deposition in ore deposits is due to small increases in Te2 fugacity reflecting restricted

supplies or short-lived release of Te at the source. Given that Te concentrations are

similar in whole rock analyses of both unaltered M1 and M2 porphyries (Hodge,

unpublished data, Appendix 9) and that pyrites from both mineralizing events contain

tellurium it seems unlikely that the difference is a function of differences in available


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Figure 5.7 X-Y plot of Au versus Te in pyrite showing a positive correlation between the two elements,

and the high concentrations of Te in Contact- and Fracture-style ore-stage pyrites. Tellurium

predominantly forms gold telluride inclusions in pyrite.

tellurium. Their reported absence from Stage II gold mineralization by Nichols (2003)

was, therefore, likely a function of sample selection.

5.2.3.2 Ore Forming Processes and Mineral Chemistry

Replacement of magnetite by pyrite and the positive correlation between

increasing pyrite abundance and increasing gold grade indicate that Stage I and Stage II

Contact-style mineralization occurred predominantly by wall-rock reaction with iron-

rich wall rock; Stage I by fluid reactions with pre-existing metamorphic magnetite

alteration, and Stage II Contact-style by reactions with primary igneous magnetite. In

contrast, the lack of evidence for oxide replacement by sulfide and the fluid inclusion

evidence for fluid immiscibility suggest that Stage II Fracture-style mineralization

occurred by phase separation, with possible contributions from other fluids.

Stage I ore-forming pyrites contain a number of different elements within the

crystal lattice. The early metamorphic magnetites in Stage I contain a number of

different elements within the crystal lattice, but also contain abundant poly-metallic

inclusions. In contrast, pyrite from Stage II Contact-style mineralization contains only

Ni and Co within its lattice, and the primary magnetite from least-altered high Mg basalt

contains only minor zircon and rare poly-metallic mineral inclusions.

It is likely that the poly-metallic composition of Stage I ore-related pyrites at

least partially reflects the inclusion composition of the pre-cursor magnetite. As

magnetite altered to pyrite, these inclusions were dissolved in the hydrothermal solution

and their elements re-incorporated as stoichiometric or non-stoichiometric substitutions

for iron within the pyrite lattice. This is consistent with the observations of Phillips et al.


99

(1986; 1988) who concluded that the composition of pyrite in the Golden Mile reflected

the composition of host rock silicates and iron oxides; i.e. dissolution of these mineral

phases led to the incorporation of chalcophile elements into the hydrothermal fluid

which subsequently precipitated pyrite. By the same principle, the relatively simple

chemical composition of Stage II Contact-style pyrite reflects the inclusion free primary

magnetite of the host high-Mg basalt. Elements such as Bi, Te, Mo, Ag, and Au, which

were absent in primary and metamorphic magnetites but present in Stage I and Stage II

Contact–style pyrites, were not contributed by sulfidation reactions with host rock oxide

minerals, but rather came from the ore fluid.

In comparison, the presence of poly-metallic sulfide inclusions within Stage II

Fracture-style gold-related pyrites most likely originated from the hydrothermal fluid, as

Stage II Fracture-style pyrite formed by phase separation and not by replacement of pre-

existing oxide minerals. This is in agreement with the findings of Carew et al. (2006)

who considered that the composition of pyrite which formed in veins without

contributions from wall-rock reactions reflected the composition of the ore fluid.

5.2.4 Comparisons with other Hydrothermal Gold Mineral Systems

There are very few published analyses of hydrothermal pyrite and magnetite

trace element geochemistry in the scientific literature, particularly from orogenic lode

gold deposits. Ho et al. (1994) analyzed pyrites from the Victory deposit in Kambalda,

by acid digest and inductively coupled plasma mass spectrometry (ICP-MS) or

inductively coupled plasma optical emission spectroscopy (ICP-OES). They reported

generally lower Co, Ni, and As, but significantly higher Cu, Zn, Mo and Au

concentrations than those observed at New Celebration. Phillips et al. (1988) analyzed

pyrites from the Golden Mile and Mt Charlotte, by atomic absorption spectroscopy

(AAS), to determine their trace element composition. They did not publish

concentration values, but demonstrated that only the chalcophile and siderophile

elements were enriched in pyrite relative to average crustal abundances. More recently,

unpublished in situ LA-ICP-MS analyses on sulfides and oxides from the New

Celebration and Golden Mile deposits by Hodge et al. (UWA internal report) illustrate

similarities between New Celebration and St Ives ore stage pyrites, but significant

differences in mineral chemistry between these deposits and the Golden Mile. Pyrites

from Golden Mile were ubiquitously high in As (up to 75,500ppm) relative to New

Celebration, and contained high concentrations of Sb (up to 5,700ppm). This is

consistent with the observations of Phillips et al. (1988), who reported Sb enrichment at


100

the expense of Bi, and Amaro (1985) who reported high As, Sb and Te and trace levels

of Bi from Golden Mile and Mt Charlotte ore-stage pyrites. Golden Mile pyrites also

contained tellurium in concentrations up to 2400ppm. Ore –stage pyrites from St Ives

had trace element concentrations more comparable with those observed at New

Celebration. They contained ubiquitous Ni and Co, with very little As (maximum

2200ppm) and Bi (up to 5000ppm) enrichment at the expense of Sb. Tellurium

concentrations at St Ives were significantly lower than those observed at Golden Mile,

but were similar to concentrations in pyrite from New Celebration.

CHAPTER SIX: HYDROTHERMAL FLUID MODEL FOR NEW CELEBRATION

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6 CHAPTER SIX: HYDROTHERMAL FLUID MODEL FOR THE NEW CELEBRATION SYSTEM

6.1 Ore Forming Processes

Gold precipitates as a function of changing physico-chemical conditions of the

ore fluid, such as temperature, fluid redox or pH. Processes that efficiently facilitate

gold precipitation include phase separation, fluid mixing or wall rock reactions (Seward,

1973, 1984; Mikucki and Groves, 1990; Mikucki, 1998), which can include sulfidation

of iron-rich host rocks (Groves and Phillips, 1987; Mernagh and Bierlein, 2008), CO2

metasomatism (Kishida and Kerrich, 1987) or fluid reduction during reactions with

graphitic host rocks (Naden and Shepherd, 1989; McCuaig and Kerrich, 1998).

6.1.1 Wall Rock Reaction

The reaction of gold-bearing hydrothermal fluids with chemically favorable host

rocks is the preferred mechanism for gold deposition in a significant percentage of

orogenic lode gold deposits, particularly where wall-rock alteration haloes host the

majority of the gold (Groves and Phillips, 1987). Increasing gold grades, therefore,

typically display a positive correlation with sulfide abundance (Goldfarb et al., 2005),

although sulfidation haloes may represent low-grade (<5 g/t Au on average, but can

locally be much higher) selvedges around higher-grade quartz-gold veins.

Predominantly, gold precipitation occurs during desulfidation reactions with Fe-rich

wall rocks according to the following reactions, modified from Phillips et al. (1996):

Fe2O3 + 4H2S0 = 2FeS2(py) + 3H2O + H2 (1)

or

(Fe2+2Fe3+)O4 + 6H2S = 3FeS2 + 4H2O + 2H2 (2)

which causes gold precipitation according to the following reaction

Au(HS)2- + H2 = Au + 2H2S (3)

Pyrite hosts gold, and higher gold grades show a positive correlation with the

increased abundance of modal pyrite in all mineralization styles at New Celebration

(Williams, 1994; Nichols, 2003) except Fracture-style. Additionally, gold is most

abundant in iron-rich wall rocks in all mineralization styles except Fracture-style.

Ankerite alteration accompanies gold mineralization and pyrite replaces magnetite.

Extensive pre-mineralization metamorphic magnetite (Williams, 1994; Hodkiewicz,


102

2003; Hodkiewicz et al., 2009) in otherwise Fe-poor intermediate porphyry host rocks

facilitated fluid-rock desulfidation reactions and consequent gold precipitation. The

majority of gold mineralization at New Celebration is considered to have resulted from

the reaction of gold-bearing hydrothermal fluids with chemically favorable host rocks.

An alternative reaction that may facilitate gold precipitation in chemically

favorable wall rocks is CO2 metasomatism (Kishida and Kerrich, 1987), which

promotes gold mineralization by releasing H2 into the ore fluid, thereby reducing the

fluid pH via the following reaction (modified from Phillips et al., 1996), which

describes the carbonation of magnetite to form Fe-carbonates:

(Fe2+2Fe3+)O4 + 3CO2 = 3Fe2+CO3 + 0.5O2 (4)

and

H2S + 2O2 = SO42- + 2H+ (5)

which destabilize the reduced gold bisulfide complexes and promote gold precipitation

by the following reaction:

2(Fe2+2Fe3+)O4 + 6HAu(HS)2 + 0.5O2 = 6Au + 6Fe2+S2 + 9H2O (6)

Ankerite is abundant in the New Celebration deposit, and is commonly

associated with type 2 ore-stage veins; however, there is no petrographic evidence to

suggest that carbonation of wall-rock magnetite was a significant process at New

Celebration (cf. Hodkiewicz, 2003).

6.1.2 Phase Immiscibility

Phase separation arises from pressure fluctuations caused by seismic-induced

fault-valve behavior (Cox et al., 2001; Sibson, 2001) or the addition of volatiles such as

CH4 or N2 to ore fluids (Naden and Shepherd, 1989). Pressure variations cause acid

volatiles such as H2S, CO2 and SO2 to partition into the vapor phase, resulting in an

increase in fluid pH, but can also cause an increase in fluid ƒO2, as reduced species

(CH4, H2S, H2) partition more readily into the vapor phase than their oxidized

counterparts (Drummond and Ohmoto, 1985; Naden and Shepherd, 1989; Mikucki and

Groves, 1990; Bowers, 1991). As these two processes can have a competing effect, the

ability of phase immiscibility to precipitate gold is dependent on the initial ore fluid pH

and ƒO2 and the magnitude of the increases in these parameters (McCuaig and Kerrich,

1998). Gold precipitation during phase separation is also influenced by the magnitude of

sulfur loss to the vapor phase. Gold in lode gold fluids is typically transported as a gold


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bisulfide (Au(HS)2-) ligand (Mikucki, 1998) and precipitates upon sulfur loss via

reactions such as:

Au(HS)2- + H+ + 1/2H2(g) = Au + 2H2S0

The addition of volatiles such as N2 or CH4 (Naden and Shepherd, 1989) can

also induce phase separation and consequent gold precipitation by increasing the vapor

field and driving the liquid-vapor solvus to higher temperatures and pressures (McCuaig

and Kerrich, 1998).

There is no evidence for phase separation in type 2 quartz veins associated with

Stage I mineralization at New Celebration. However, the presence of liquid-rich and

vapor-rich end members in some pseudosecondary clusters or trails, total

homogenization into liquid and vapor at the same temperature of at least some of these

inclusions, and variable bulk compositions and molar volumes within individual trails

or clusters of H2O-NaCl-CO2±CH4 inclusions in type 3 veins (Fig. 4.4, Chapter 4)

indicate that at least intermittent phase separation did occur during Stage II

mineralization. The extent to which fluid immiscibility influenced gold mineralization

during Stage II is unclear, as free gold within type 3 veins is rare and the evidence for

significant phase immiscibility is limited. However, the negative sulfur isotopic

composition (-10.6‰ to -3.2‰, refer to Table 5.1 and Figure 5.1, Chapter 5) and spread

of values observed in gold-associated pyrite suggests that phase separation was at least a

partial contributor to gold mineralization during Stage II (cf. Hodkiewicz et al., 2009).

6.1.3 Fluid Mixing

Fluid mixing destabilizes gold in solution either by the addition of a cooler fluid

or by changing the pH or oxygen fugacity of the ore fluid through the addition of either

a more oxidized or more reduced fluid and may result from the mixing of two externally

derived fluids or back-mixing of internally derived end-member fluids (cf. Uemoto et

al., 2002). A number of authors consider that fluid mixing is unlikely in orogenic lode

gold deposits given the uniform fluid conditions observed in broadly disparate deposits

(McCuaig and Kerrich, 1998), however mixing of meteoric fluids with deeply derived

hydrothermal fluids has been proposed for some sub-greenschist facies deposits (e.g.

Hagemann et al., 1994; Gebre-Mariam et al., 1997).

A plot of homogenization temperature vs. salinity of aqueous-carbonic fluid

inclusions assemblages trapped in type 2 and type 3 veins (Fig. 5.3, Chapter 5) does not

indicate that fluid mixing with cooler meteoric water was a significant fluid process (cf.


104

Wilkinson, 2001), and the depth of formation at meso- to hypozonal crustal levels (6 to

14 km depth) would also suggest that this was unlikely. However this relationship does

not take into account the possibility of mixing aqueous or aqueous-dominated fluids

with one or more gas-rich fluids. Neumayr et al. (2008) proposed that gold

mineralization at St Ives formed due to a progressive change of redox conditions

brought about by mixing a reduced, vapor-rich lower crust or mantle derived fluid with

a more oxidized fluid derived locally from felsic and intermediate granitic stocks, and

argued that this mechanism would also explain the presence of gold-bearing sulfides

with depleted sulfur isotopic values. At New Celebration, CO2 –rich fluid inclusions in

type 3 quartz-carbonate veins indicate the presence of carbonic fluids in the

hydrothermal system at some point, so in theory, there may have been mixing between a

CO2-rich fluid and the H2O-CO2 ore fluids. However the temporal relationship between

CO2-rich inclusions and the ore-related inclusions is unclear. The CO2-rich inclusions

are observed in the same veins as the gold related inclusions, but not in the same

inclusion trails or clusters as the H2O-CO2 inclusions. The petrographic and genetic

relationships between these two fluids therefore cannot be determined. Alternatively,

the addition of CH4 to the ore fluids would trigger gold precipitation by initiating phase

separation, and there is abundant evidence (see Chapter 4, Figure 4.1a) for long-lived

methane dominated fluids within the New Celebration hydrothermal fluids. The

majority of aqueous-carbonic fluid inclusions measured in type 2 and type 3 veins,

however, contained only trace amounts of methane, and there was no evidence for

methane-rich fluid inclusions in the same clusters or trails as the gold-related inclusions

in either vein type. Based on these observations, it does not appear that fluid mixing was

a significant factor in gold mineralization.

6.2 Constraints on Fluid and Metal Sources

As with many orogenic lode gold deposits around the world the source of the

hydrothermal fluids and metals at New Celebration remain unconstrained. Potassium,

Mg and Ca over Na ratios, and high base metal concentrations in Stage II related fluids,

relative to Stage I, indicate that at least two different gold-bearing fluids were

responsible for gold mineralization at different times. Traditional models for Archean

orogenic lode gold deposits invoke a hydrothermal ore fluid generated during

metamorphic devolatilization of carbonate-bearing mafic rocks at the greenschist-

amphibolite facies transition (Phillips and Groves, 1983; Powell et al., 1991). The 34S

values of Stage I ore-related pyrites, which range between -7.6‰ and +3.2‰, and ore


105

fluid K/Ca ratios <1 are consistent with a non-magmatic (cf. Haynes and Kesler, 1988),

likely metamorphic fluid source, however, depleted 34S values of ore-stage pyrites and

contrasting hydrothermal fluid chemistry suggest an alternative fluid source for Stage II

mineralization. Ridley and Diamond (2000) suggested that the only viable fluid sources

for the formation of orogenic gold deposits were those derived from metamorphic

devolatilization (Powell et al., 1991) or magmatic fluid derived from granitoids (e.g.

Burrows and Spooner, 1986; Cameron and Hattori, 1987; Mueller et al., 1991; Qiu and

McNaughton, 1999; Mueller, 2007). Other potential fluid sources include the deep

circulation of seawater (Thébaud et al., 2006), modification of CO2-rich mantle fluids

during lower crustal granulite facies metamorphism (Cameron, 1988, 1993),

devolatilization of the crust during prograde metamorphism (Powell et al., 1991), and

devolatilization of felsic magmatic crust (Burrows and Spooner, 1986; Cameron and

Hattori, 1987; Mueller et al., 1991; Qiu and McNaughton, 1999) and/or shoshonitic

lamprophyres (Rock and Groves, 1988a; Rock et al., 1989).

Fluids with a surface (meteoric and/or seawater) origin have been reported from

a number of orogenic lode gold deposits (e.g. Racetrack, Gebre-Mariam et al., 1993;

Wiluna, Hagemann et al., 1994; Golden Kilometre, Gebre-Mariam et al., 1997) and

greenstone belts (e.g. Warrawoona Syncline, Pilbara Craton, Thébaud et al., 2006)

although most orogenic gold deposits are considered to have formed too deep in the

crust for significant surface water influx. In most cases where surface waters were

reported, they were interpreted to have infiltrated the hydrothermal system late in its

evolution (e.g. Taylor et al., 1991) and did not represent primary ore fluids. Exceptions

include Wiluna, where Hagemann et al. (1994) proposed a two-fluid model, in which

shallow surface waters mixed with deeply derived ore-fluids and early stage gold-

pyrite-arsenopyrite mineralization precipitated in equilibrium with the mixed fluid, and

Racetrack, where Gebre-Mariam (1997) proposed mixing of the ore fluid with

infiltrating surface waters as the mechanism by which gold precipitated.

Cameron (1988) proposed upward streaming of mantle CO2 along crustal scale

shear zones during granulite facies metamorphism of amphibolitic lower crust as a

mechanism by which large volumes of fluid and metals could have been transported to

the middle crust to form orogenic lode gold deposits. This was based on the apparent

contemporaneity of lode gold formation and crustal thickening with associated granulite

formation during the Archean, the association of juvenile 13C haloes with gold-related

major crustal breaks, and depletion of large ion lithophiles (LIL) in the lower crust.


106

Whether CO2 flux is the cause of granulite facies metamorphism, however, has been

questioned by Hoernes and van Reenen (1992), as has the ability of granulite facies

metamorphism to induce LIL depletion (Knudsen and Andersen, 1999). Further, studies

of tectonic evolution and gold mineralization in the Yilgarn have concluded that

carbonate alteration with juvenile mantle isotopic signatures associated with the BLFZ

were not associated with the gold mineralization, but rather, predated it (e.g. Bartram

and McCall, 1971; Barley and Groves, 1987; Norris, 1990).

Devolatilization of shoshonitic lamprophyres during crystallization has been

proposed as a possible source of gold in orogenic lode gold deposits (Rock and Groves,

1988a, b; Rock et al., 1989), based on the close spatial association between lamprophyre

dikes and gold mineralization observed in Archean greenstone terranes (Kerrich and

Wyman, 1994), e.g. Golden Mile (Mueller et al., 1988; McNaughton et al., 2005), New

Celebration (Williams, 1994) and Darlot (Kenworthy and Hagemann, 2005).

Lamprophyres, however, are not intrinsically Au-rich, nor are they volumetrically

significant in orogenic gold deposits, and their temporal and spatial relationship is

considered to reflect formation in a common geodynamic setting (Kerrich and Wyman,

1994), rather than a viable source for gold mineralization (e.g. Darlot, Kenworthy and

Hagemann, 2005) in orogenic lode gold deposits.

A number of authors (Burrows et al., 1986; Cameron and Hattori, 1987) have

proposed the devolatilization of felsic magmas during crystallization as a possible

source of fluids and/or metals for orogenic lode gold mineralization, based on C and S

stable isotope compositions, petrographic and isotopic evidence for oxidized ore fluids

and similarities between lode-gold and granite-hosted ore deposits. Potential sources

include tonalite-trondhjemite-granodiorite (TTG) suites (Burrows and Spooner, 1987),

oxidized alkaline magmas (Cameron and Hattori, 1987), evolved igneous complexes

(Qiu and McNaughton, 1999), low-Ca granites (Blewett and Hitchman, 2006) and

reduced Sn-W granites (Thompson et al., 1999). Opponents of the magmatic fluid

model cite the absence of outcropping granites coeval with gold mineralization, and the

expected production of high-salinity aqueous fluids from crystallizing magmas as the

main reasons against a granitic source, however, a number of authors have put forth

compelling arguments supporting a magmatic fluid model. Modeling of hydrothermal

fluid evolution during crystallization of granitic magma by Cline and Bodnar (1991)

demonstrated that high salinity fluids, such as those recorded in porphyry-type deposits,

were not predicted when crystallization took place at pressures above 1.3kbars. Further,


107

Eggler and Kadik (1979) proposed that the exsolution of mixed H2O-CO2 fluids from

granites crystallizing at solidus temperatures was entirely feasible at pressures above

3kbar, due to the increased solubility of CO2 at higher pressures. Recent work by

Landtwing et al. (2002) and Redmond et al. (2004) on the Bingham Canyon porphyry

copper deposit reported that the earliest magmatic fluid, prior to phase separation at

higher crustal levels, was single-phase, CO2 bearing, and of low to moderate (2-7 wt.%

NaCl equiv.) salinity. Mair et al. (2006) also reported low-salinity magmatic fluids from

the Scheelite Dome intrusion related gold deposit in the Tintina gold belt, Yukon.

The major argument rejecting a magmatic source for Archean orogenic lode-

gold ore fluids is the lack of outcropping coeval granites in or near most deposits

(Groves, 1993). Recent work by Bucci et al. (2002; 2004), however, indicates a genetic

relationship between gold mineralization and temporally and spatially related granitoid

magmatism at the Chalice deposit in the Yilgarn Craton. At New Celebration, felsic

intrusions host gold mineralization, which although not large enough themselves to

generate the fluid volumes required for a deposit the size of New Celebration, must

reflect an underlying granitic magma source at depth. This is consistent with the recent

findings of Mueller (2007) who described biotite and sericite alteration and magnetite-

hematite-pyrite gold lodes, which are mineralogically identical to wall rock alteration

described for parts of the Golden Mile (Clout et al., 1990; Bateman and Hagemann,

2004), and for the New Celebration (Norris, 1990) and Kambalda (Watchorn, 1998)

deposits, in his paper on the association between Cu-Au endoskarns and high-Mg

monzodiorite-tonalite intrusions at Mt Shea, located approximately halfway between the

Golden Mile and New Celebration deposits. Mueller (2007) concluded that the Mt Shea,

and by inference, Golden Mile and possibly other deposits spatially associated with the

BLFZ, formed from oxidized magmatic fluids generated from buried sanukitoid series

plutons.

Seismic investigations of the crustal structure of the Yilgarn craton (e.g. Goleby

et al., 2000; Goleby et al., 2002; Stolz et al., 2004; Blewett and Hitchman, 2006; Goleby

et al., 2006) identified large volumes of low-Ca granite underlying the craton. Recent

seismic surveys at St Ives gold mine, located approximately 30 kilometers south of New

Celebration along the Boulder Lefroy Fault Zone, indicate that large granite bodies are

localized within the greenstone belts (Stolz et al., 2004), although the timing of these

granites with respect to gold mineralization is poorly constrained. Neumayr et al. (2008)

consider fluids derived from these granites to be critical to their fluid mixing model for


108

the St Ives gold deposits. More specifically, Blewett and Hitchman (2006) identified a

number of domal structures, two of which are underlain by granite laccoliths or sills that

correspond to the locations of the world class St Ives and Kanowna Belle deposits.

6.3 Integrated Model for the Evolution of the New Celebration

Gold Mineral System within the BLFZ

Detailed fluid inclusion, sulfide and oxide geochemistry and sulfur isotope

analyses of veins, sulfides and oxides associated with pre- syn- and post-gold

mineralization hydrothermal events point towards a complex hydrothermal fluid system

through time within the western segment of the BLFZ. Combining the structural,

hydrothermal alteration and fluid chronology outlined in chapters 3-5, a three-stage

model for the development of the New Celebration gold deposits (Fig 6.1) is proposed.

6.3.1 Early Evolution (D1-D2)

Subsequent to the emplacement of the regional volcano-sedimentary sequence

and N-S directed regional D1 deformation but prior to the onset of peak metamorphism

and gold mineralization at New Celebration, formation of a proto-BLFZ was initiated

by the development of north-south-striking, east and west-dipping discrete thrust faults

during regional D2 east northeast-west southwest-oriented shortening and crustal

thickening (Weinberg et al., 2005). At New Celebration, regional D2 manifested in the

upright tilting of conformable stratigraphic units (Nichols, 2003).


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Figure 6.1 Hydrothermal fluid flow model for the Boulder Lefroy Fault Zone (BLFZ) at New Celebration.

A. During early D3NC ENE-WSW shortening, M1 plagioclase porphyry is emplaced into the BLFZ and

metamorphosed, which included the development of metamorphic magnetite. Methane dominated fluids

of possible deep crustal or mantle origin circulate through the fault zone. B. Stage I gold mineralization

occurred at or around peak metamorphism by wall rock sulfidation of magnetite (i) in M1 porphyries

from CO2 dominated fluids of likely metamorphic origin. C. M2 quartz-feldspar porphyries were

emplaced in the BLFZ. Stage II gold mineralization occurred due to a combination of fault-valve induced

phase separation of CO2-bearing magmatic fluids and sulfidation of iron oxides at the contact between

high-magnesium basalt and M2 porphyry; D. The fault experienced a period of uplift and erosion during

which highly saline fluids potentially of magmatic origin were emplaced and the fault returned to steady

state with long-lived methane-rich fluids again dominating.

6.3.2 Early D3NC

Reactivation of the early thrust faults during early D3 ESE-WNW-directed

shortening led to sinistral shearing and the linking of these faults to form a coalescent

multi-stranded major crustal fault system (Weinberg et al., 2005) extending from

Kalgoorlie to Kambalda. The presence of deformed lamprophyres adjacent to and

within the BLFZ at New Celebration (Williams, 1994) suggest that at some point the


110

fault had a connection to the deep crust or mantle (cf. Rock and Groves, 1988a; Rock

and Groves, 1988b; Rock, 1990).

Sinistral, oblique-slip, west-block-down to the south-southwest movement

characterized D3 deformation at New Celebration and resulted in the development of a

penetrative north-northwest trending, steeply west-southwest dipping S3NC foliation

(Nichols, 2003). Emplacement of the M1 intermediate plagioclase-phyric porphyritic

dike into the fault zone coincided with the onset of D3NC and peak metamorphism, and

led to the development of metamorphic magnetite in an otherwise iron-poor intrusive

rock of intermediate composition. Type 1 foliation parallel quartz veins display highly

deformed and recrystallized quartz, suggesting formation and deformation prior to the

onset of peak metamorphism. Type 2 quartz-calcite veins emplaced during the early

formation of the BLFZ trapped methane and aqueous-carbonic fluid inclusions in the

calcite margin between 270 °C and 500 °C and pressures between 1.1 and 3.1 kbars

(Fig. 6.1a). Development of the BLFZ as a regionally extensive deep-crustal structure

likely coincided with the introduction of potentially mantle-derived methane into the

hydrothermal system at New Celebration, evidenced by primary, early, pre-gold

methane inclusions in type 2 quartz-carbonate veins.

6.3.3 Stage I Gold Mineralization (D3NC)

Stage I mineralization took place after peak metamorphism during D3NC

deformation (Witt, 1993a; Copeland, 1998; Nichols, 2003). Stage I Au formed within

ductile, oblique-slip, shear-related fabrics in magnetite-altered intermediate plagioclase

(M1) porphyry and mylonitized mafic schist from gold-bearing, aqueous-carbonic

fluids characterized by low- to moderate salinity (2-8 wt.% equiv. NaCl), low to

medium XCO2 (0.03-0.3) and trace methane (XCH4 = 0.0-0.04). Single inclusion laser

ablation analyses indicate that the ore fluid was Na-Ca dominant, with subordinate Mg

and K, and K/Ca ratios <1, consistent with a non-magmatic (cf. Haynes and Kesler,

1988) likely metamorphic fluid origin, and contained ppm level Au, Fe, Cu, Zn, and As.

Formation temperatures and pressures ranged between 330 °C and 500 °C and 2.4 and

4.2 kilobars, respectively, which corresponds to crustal paleodepths between 10 and 14

kilometers (cf. Brown and Hagemann, 1995). The strong positive correlation between

increasing gold grade and modal pyrite abundance, and the replacement of metamorphic

magnetite with pyrite in M1 porphyries and mafic schists indicate that gold precipitated

by wall rock reaction between sulfur-bearing hydrothermal fluids and magnetite-bearing

wall rocks. The lack of phase ratio variability in gold-bearing fluid inclusion trails and


111

clusters in type 2 quartz-calcite veins (Fig. 4.1, Table 4.1, Chapter 4), and the lack of

free gold in these veins indicate that phase immiscibility was not a factor for gold

precipitation during Stage I at New Celebration.

6.3.4 Stage II Gold Mineralization (Late D3NC-Early D4NC)

Stage II mineralization occurred post-D3NC (Nichols, 2003) during brittle

reactivation of the BLFZ at the end of D3NC and during early D4NC (Nichols et al.,

submitted). Stage II gold mineralization formed within the M2 porphyry and at the

contact between the porphyry and high magnesium basalt (Fig. 3.5. Chapter 3) and it is

likely that the emplacement of the porphyry into the fault facilitated fluid movement by

creating pore space along the contacts. Stage II gold mineralization formed from a low

salinity (1.1 to 7.7 wt. % NaCl equiv.) aqueous-carbonic fluid with variable carbon

dioxide contents (XCO2= 0.03 to 0.76) and trace methane. Stage II ore-forming fluids

were Na-Mg-K dominant, with lesser Ca (K/Ca >1), consistent with a magmatic fluid

source (cf. Haynes and Kesler, 1988) in addition to ppm level Au, Fe, Cu, Pb, Zn, and

As. Interpretation of fluid inclusion microthermometry indicate that Stage II gold

mineralization at New Celebration occurred at temperatures and pressures between 280

and 360° C, and 1 to 3.5 kbars, which corresponds to formation depths between 4 and

10km. Temperatures and pressures recorded from Stage II are shallower and cooler than

those recorded from Stage I (Fig. 4.6, Chapter 4), suggesting that a period of uplift and

erosion may have separated the two mineralizing events. Replacement of wall rock

oxides by pyrite in high-Mg basalt along the contacts of the porphyry indicate that

sulfidation reactions were a significant component in forming Stage II gold, at least for

Contact-style mineralization, and fluid inclusion evidence suggests that phase separation

and/or fluid mixing were at least partial contributors to gold mineralization during Stage

II.

6.3.5 Post-gold evolution (>D4)

Secondary post-gold fluid inclusions in types 2 and 3 quartz veins (Fig. 4.1f)

record at least three distinct phases of fault zone reactivation at New Celebration. Low

salinity aqueous fluids without dissolved CO2 had salinities between 0.8 and 13.8

weight percent NaCl equivalent and densities between 0.76 and 1.04 g/cm3. In type 2

quartz veins, inclusions homogenized to liquid between 173 and 351 °C, whereas in

type 3 quartz veins, final homogenization were recorded at much lower temperatures,

between 90 and 152 °C. Calculated isochores indicate that these inclusions were trapped


112

at about 260 °C and a maximum of 3.5 kbars (Figs. 4.5, 4.6, Chapter 4). High salinity

aqueous inclusions in secondary trails in both types 2 and 3 veins had salinities ranging

between 18.4 and 23.2 equivalent weight percent NaCl and densities between 1.09 and

1.17 g/cm3 (Table 4.1, Chapter 4). These inclusions homogenized to liquid between 55

°C and 118 °C. Laser Raman analysis indicated that the petrographically latest observed

inclusions comprised almost pure methane with minor N2 and trace C2H6 and C3H8.

These inclusions homogenized to liquid at around -90 °C and had densities around 0.26

g/cm3. Isochores calculated from the high salinity aqueous inclusions, indicate that they

were trapped at temperatures between 100 and 180 °C and pressures estimated to be

between 0.4 and 1.0kbars (Fig. 4.6). These very low temperatures and pressures indicate

emplacement in a very low P-T tectonic regime, suggesting significant uplift and

erosion took place during the final reactivation stages of the BLFZ.

6.4 Comparisons with other Orogenic Lode Gold Systems

Table 6.1 summarizes the characteristics of orogenic lode gold deposits

including granitoid-hosted orogenic lode gold deposits, intrusion-related gold deposits

and orogenic lode gold deposits hosted within first-order crustal scale fault systems

world wide, as described by a number of authors (Kerrich and Cassidy, 1994; Groves et

al., 1998; McCuaig and Kerrich, 1998; Hagemann and Cassidy, 2000; Goldfarb et al.,

2001; Groves et al., 2003). The following sections compare the New Celebration

deposit with other orogenic lode gold deposits around the world.

6.4.1 Host Rocks and their Role in Gold Precipitation

Stage I mineralization at New Celebration is located within M1 intermediate plagioclase

phyric porphyritic intrusions, whereas Stage II mineralization is hosted in the hanging

wall and foot wall contacts between M2 quartz-feldspar porphyry and tholeiitic basalt,

and within the M2 porphyry. Felsic intrusions commonly host orogenic lode gold

mineralization in the Abitibi subprovince of eastern Canada (Hodgson and Troop,

1988), and granitoids host many orogenic lode gold deposits in Australia (e.g. Granny

Smith (Ojala et al., 1993; Ojala, 1995; Ojala et al., 1995), Lady Bountiful (Bartch, 1990;

Cassidy and Bennett, 1993), Chalice (Bucci et al., 2002; Bucci et al., 2004)). In the

Yilgarn craton, however, iron-rich mafic lithologies are by far the most volumetrically

significant host of orogenic lode gold deposits (Groves, 1990). The M1 intermediate

plagioclase porphyritic intrusions and mylonitized intrusions that host Stage I

mineralization are not intrinsically iron-rich; however, they do contain abundant pre-


113

mineralization metamorphic magnetite. This is, besides the structural control, likely a

key contributing factor in the location of the New Celebration deposits, as petrographic

relationships between pyrite and magnetite in the New Celebration ore zones indicate

that most of the gold at New Celebration formed by the replacement of wall rock

magnetite by gold-bearing pyrite. This is compatible with the accepted theory that the

most common precipitation mechanism for gold at most orogenic lode gold deposits is

precipitation by wall rock sulfidation of iron-rich lithologies (Groves and Phillips, 1987;

Colvine et al., 1988; Groves et al., 2003; Mernagh and Bierlein, 2008)}.

Felsic porphyritic intrusive rocks and the contact between the porphyry and

high-Mg basalt host Stage II mineralization, with the emplacement of the porphyry

stock into the fault zone likely facilitated contemporaneous fluid flow up the fault and

into the depositional site. The correlation between wall rock pyrite abundance and

increasing gold grade (Williams, 1994), and the replacement of iron oxides by pyrite in

the high-Mg basalt indicate that wall rock sulfidation was the major process forming

Contact-style gold during Stage II. However, gold that precipitated in brittle fractures

within the felsic porphyry did not form by wall rock sulfidation reactions. Firstly, there

is not enough iron in the felsic porphyry to facilitate such reactions, as evidenced by the

lack of replacement of oxides by pyrite, and secondly, evidence for phase separation in

type 3 quartz veins, which indicates that at least some of the gold precipitated by

unmixing. Phase separation was likely caused by failure-induced pressure reduction (cf.

Cox et al., 1995; Sibson, 2004) during the intense non-coaxial deformation within the

shear zone, which resulted in extensive brittle fracturing of the felsic porphyry (Norris,

1990), during late D3NC and D4NC.

6.4.2 Methane-rich and Highly Saline Aqueous Fluids

The aqueous-carbonic, low to moderate salinity ore-forming fluids at New

Celebration are typical and representative of orogenic lode gold fluids worldwide

(Hagemann and Cassidy, 2000). The presence of methane (± trace hydrocarbon)

inclusions, however, although not unique, is not a feature of typical orogenic lode gold

deposits. Polito et al. (2001) reported methane inclusions from the Junction deposit near

Kambalda and postulated that they were not part of the ore fluid, but were introduced

later. Methane-dominant fluids both pre- and post-date the ore-related fluids at New

Celebration and, if they are of the same source, appear to be very long lived within the

fault zone. The origin of the methane-dominated fluids at New Celebration is unknown;

however, in deposits such as the Paringa lode (Golden Mile), Lancefield (Laverton) and


114

Table 6.1 Summary of hydrothermal fluid characteristics from orogenic gold deposits, granitoid-hosted gold deposits, intrusion related gold deposits and orogenic deposits hosted in first

order fault zones. ab=albite, ank=ankerite, aspy=arsenopyrite, bio=biotite, bis=bismuthinite, cb=carbonate, cc=calcite, chl=chlorite, cpy=chalcopyrite, fl=fluorite, fuch=fuchsite, ga=galena,

hm=hematite, il=ilmenite, kf=K feldspar, mo=molybdenite, ms=muscovite, mt=magnetite, po=pyrrhotite, py=pyrite, qz=quartz, ru=rutile, sch=scheelite, sid=siderite, sph=sphalerite,

tell=tellurides, tlc=talc, tm=tourmaline, van=vanadian mica.

Orogenic Lode Gold Deposits Granitoid-Hosted Orogenic Lode Gold Deposits Intrusion-Related Gold Deposits Deposits in First Order

Fault Systems New Celebration Golden Mile Victory Hollinger-McIntyre Sigma Lamaque Lady Bountiful Granny Smith Porphyry Kidston Timbarra Kerr-Addison

Resources (tonnes Au)

78 2400 265 1000 290 141.8 11.4 49.5 10.6 94 12.4 340

Mineralization Age

Oroya: 2638±6 Fimiston: 2630 Mt Charlotte: 2600

2627±14 <2679 2682±8 (zircons) 2682±8 (rutile) 2579±9 (muscov) 2596±33 (scheel)

2648±6 2665±4 2667±4 332 2675-2670

Host Rocks tholeiitic basalt intermediate plagioclase-phyric porphyry quartz-feldspar porphyry

Golden Mile Dolerite Defiance Dolerite Paringa Basalt Tripod Hill Komatiite Kapai Slate

tholeiitic basalt andesitic flows volcaniclastic rocks subvolcanic porphyritic diorite

quartz-monzodiorite /granodiorite stock Intermediate-mafic volcanic rocks

biotite granodiorite gabbronorite Mt Pleasant mafic sill

quartz diorite-granodiorite sedimentary ± volcanic rocks

biotite ± hornblende quartz monzonite felsic volcanic rocks

metamorphic rocks, granodiorite, rhyolite porphyry

leucomonzogranite

komatiite and Fe-tholeiite schists diorite dykes

Crustal Depth Stage I: 10-15km Stage II: 4-10km

<6km 5-12km <5-7km <5-7km <5-7km <5-8km 5-10km 3.5km <4km

Metamorphic Grade

mid-upper greenschist

greenschist upper greenschist-lower amphibolite

lower-mid greenschist

greenschist greenschist lower-mid greenschist



greenschist

Mineralization Timing

post-peak metamorphism

Oroya and Fimiston: syn-peak metamorphism Mt Charlotte: post-peak metamorphism


post-peak metamorphism?




post-contact metamorphism



Structural Regime brittle-ductile to brittle

brittle-ductile to brittle brittle-ductile brittle-ductile brittle brittle brittle in granitoid brittle in granitoid

brittle-ductile brittle-ductile

Deposit Style Stage I: wall rock hosted Au in sheared and mylonitized intermediate porphyries and basalts Stage II: brittle qz-ser-py veins in felsic porphyry

Fimiston: brittle-ductile fault-hosted lodes Oroya: breccia Mt Charlotte: sheeted veins and stockworks

brittle-ductile shear zones, quartz breccia zones and brittle quartz vein arrays

quartz-carbonate vein and wall rock hosted Au

quartz veins quartz veins sets/stockworks

massive to laminated quartz veins ± breccia zones

conjugate fracture/vein sets, breccias, shear zones

shear zone ± quartz veins

breccia hosted disseminated and veins

vein hosted quartz stockwork and disseminated pyrite


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Major Structures BLFZ: NNW trending sinistral shear (D3-D4)

BLFZ: NNW-SSE trending zone of steep E and W dipping thrust ramps (D2) NNE trending dextral en echelon shear zone (D3-D4)

BLFZ: NNW trending sinistral shear (D3-D4) and late D3 extension

HSZ: NE trending steeply dipping shear with reverse oblique (dextral) movement

CTZ: EW trending steep reverse fault (D2); transcurrent (D3)

E-W striking, steeply N dipping sinistral strike slip fault

N-S striking, moderately E dipping reverse shear zone, granitoid contact

NNW striking, shallow E dipping sinistral reverse shear

CTZ: EW trending steep reverse fault (D2); transcurrent (D3)

Vein Mineralogy

Silicate minerals Stage I: qz-cb Stage II: qz-ser

Fimiston: qz Oroya: Mt Charlotte: qz-cb-sch

qz-cb qz-ank-ab-sch-chl-tm

qz-tm-cc-chl-sch qz-tm-ank-cc-ms±chl

qz-cc-ms±chl±ru qz-ank±ms±ru qz-ank-ms±chl±ru±tm

qz-mus-cc-fl-chl

qz-cb

Ore minerals Stage I: py±cpy±gn Stage II: py

Fimiston: py-cpy-sph-ga-tell-teld-my Oroya: py-cp-sph-po-tell Mt Charlotte: py

Py, po sph-cpy-po-ga-tell-bi-Au

py-Au-tell py, po, cpy, sch, Au, tell

Stage I: py±po±cpy Stage II: py-tell-ga±cpy±sph

py±po±cpy±ga±sph±apy±tell

py-cpy-ga-mo py-po-sph-cpy-mo-gn-aspy-bis

aspy-mo-tell py

Wall rock alteration

Stage I: bi-ank-ser-py Stage II: ank-ser

Fimiston: ser-ank-sid-qz-hm-py-tell Oroya: van-ank-qz-sid-tell-py-mt-hm-cc-ab-aspy Mt Charlotte: chl-ab-ser-ank-il-ru-py-po

Basalt and dolerite: qz–ab–ank–ser–py-(bio) Komatiite: trem–bio–tlc–qz–py–dol Kapai Slate: qz–ab–ser–py–ank-(mt–cl)

qz-ank-ab-ser±chl±cc

chl-cb-ser-ab qz-ab-carb-py-mu±chl±bt

qz-ab-ms-cc±chl±py±ru

qz-ms-ank-ab-py±ru±chl±kf

qz-ab-ms-ank-py-ru±chl±kf±tm±hm

qz-ser-cb mus-chl-cb-Au

fuch-cb, cb-si, ab

Metal Association Au-Ag-Bi-Te-Pb-Ba-Zn-As-Sr-Sb

Fimiston: Au-As-Sb-Te-V-Ba Oroya:Au-V-Te-W-Sb

Au-Ag, Te Au-W-Te-Bi-As-Ba Au-W-Cu-Pb Au-Ag-As-Te-Bi-W-Pb

Au-Ag-As-Sb-Bi-Te-W

Au-Ag-As-Mo Zn-Cu-Mo-W-Pb-As-Bi-Te-Sn

Au-Bi-Ag-Te-As-Sb-Mo-Sn

Au-Ag-W-As-Sb

Fluid Chemistry H2O-CO2-NaCl±CH4

Fimiston: H2O-CO2-NaCl±CH4 Oroya: H2O-CO2-NaCl-CH4 Mt Charlotte: H2O-CO2-NaCl-CH4

H2O-CO2-CH4-N2 H2O-CO2-NaCl-CH4

H2O-CO2-NaCl and H2O-NaCl

CO2-H2O-NaCl±CH4

CO2-H2O-NaCl±CH4

CO2-H2O-NaCl±CH4

CO2-H2O-NaCl H2O-CO2-NaCl CO2 and H2O-NaCl

XCO2 Stage I: 0.03-0.3 Stage II: 0.03-0.3

Fimiston and Oroya: ~ 0.2 Mt Charlotte: up to 0.5

0.98-1.00 0.03-0.24 0.15-0.30 0.06-0.19 0.21-0.59 moderate 0.1

XCH4 Stage I: Stage II:

0.00-0.05 <0.06 0.10-0.30 0


116



Salinity Stage I: 2.0-8.0 wt.% NaCl equiv. Stage II: 1.5-7.5 equiv.wt.% NaCl

Fimiston and Oroya: <6 wt.% NaCl equiv. Mt Charlotte: 2.0-5.5 equiv.wt.% NaCl

8-9 wt.% NaCl equiv.

6 wt.% NaCl equiv. <10 wt.% NaCl equiv. (aq-cb) 25-34 wt.% NaCl equiv.

low salinity 7-10 wt.% NaCl equiv.

<2.0 wt.% NaCl equiv.

low-moderate 2-10 wt.% NaCl equiv.

5-7 wt.% NaCl equiv.

pH 6.0-8.0 5.3-5.6 5.9 5.0 - 6.0

Temperature Stage I: 330-500 °C Stage II: 280-360 °C

Fimiston and Oroya: 250-350 °C Mt Charlotte: 120-440 °C

370-390 °C 380-480 °C (no phase separation) 277±48 °C (phase separation)

285-395 °C (aq-cb) 60-295 °C (aq)

~400 °C Stage I: 300±50 °C Stage II: 250±50 °C

325±50 350±50 °C 170-350 °C 270-300 (isotopic equilibrium) 300-350

Pressure Stage I: 2.4-4.2 kbars Stage II: 1.5-3.5 kbars

Fimiston: 1.0-2.2 kbar Oroya: 1.0-2.0 kbar Mt Charlotte: 1.5-2.3 kbar

1.7-2.0 kbar 1.8-2.6 kbars (no phase separation) 0.8-1.6 kbars (phase separation)

1.5-2.5 kbar Stage II: ~0.5-2.0 kbar

0.7-2.6 kbar ~2.0kbar

δ34S Stage I: -6.0 to +3.9‰ Stage II: -8.7 - +2.2‰

Fimiston: -10.0 - +12.6‰ Oroya: -3.1 - +5.8‰ Mt Charlotte: -4.2 - +4.3‰

-6.3-+5.1‰ -0.7 - +7.0‰ -1.1 - +9.5‰ +0.3 - +4.5‰ -10.2 - +10.0‰

Gold deposition mechanism

Stage I: wall rock sulfidation Stage II: phase separation and fluid mixing

Fimiston: Phase immiscibility, sulfidation, mixing Oroya: Phase immiscibility Mt Charlotte: wall rock sulfidation

Phase immiscibility, wall rock reaction

phase separation? wall rock reaction

phase separation wall rock reaction Stage II: Phase separation

sulfidation ± phase separation

fluid-wall rock interaction

phase separation Flow Ore: Wall rock sulfidation of tholeiite and albitite Green Cb Ore: Phase separation

References Nichols (2003), Weinberg et al. (2005), this study

Mikucki and Heinrich (1993), Ho (1987), Ho et al. (1990), Mernagh (1996), Golding et al. (1990), Clout (1989), Hagemann et al. (1999), Phillips (1986), Larcombe (1912), Bateman and Hagemann (2004), Hagemann and Cassidy (2000), Weinberg et al. (2005)

Hodkiewicz, (2003); Hodkiewicz et al. (2009), Clark et al., (1989), Neumayr et al., (2008), Palin and Xu, (2000), Petersen et al., (2006)

Hagemann and Cassidy (2000), Smith et al. (1984), Wood et al. (1986a, b), Spooner et al. (1987), Channer and Spooner (1991), Hagemann and Brown (1996)

Robert and Brown (1986), Robert and Kelly (1986)

Burrows and Spooner (1989)

Cassidy (1992), Cassidy and Bennett (1993), Hodkiewicz (2003)

Ojala et al. (1993, 1995), Ojala (1995)

Allen (1987), Cassidy (1992), Hill (1992)

Baker and Andrew (1991), Baker and Tullemans (1990), Thompson et al. (1999)

Mustard (2001), Simmons et al. (1996)

Kishida and Kerrich (1987), Robert and Poulsen (1997)


117

Water Tank Hill (Kambalda) they result from fluid reactions with carbonaceous

sedimentary rocks or the devolatilization of graphitic rocks (Ho, 1987). Black shales,

which are a ubiquitous component of the Kalgoorlie Terrane may be the source of the

methane-dominated fluids, however, black shales do not outcrop within the New

Celebration open pits or underground workings, or any of the adjacent satellite deposits

and therefore are unlikely to be volumetrically significant enough in the immediate

vicinity to contribute to the methane dominated fluids.

Polito et al. (2001) postulated that the presence of methane at the Junction

deposit in Kambalda was the result of Fischer-Tropsch type synthesis of light

hydrocarbons from reactions between a CO2-rich fluid, hydrogen, and titanomagnetite

or ilmenite in the Junction dolerite under reduced conditions. Such reactions have also

been invoked to account for the presence of methane and other hydrocarbons in

orogenic lode gold deposits in Canada (Graney and Kesler, 1995) and South Africa

(Bray et al., 1991; de-Ronde et al., 1992). Sensitive gas chromatographic analyses of

light hydrocarbons aside from methane and ethane were outside of the scope of this

study, however, laser Raman analyses detected only trace amounts of ethane and

propane in monophase CO2-CH4 inclusions. Given that other evidence such as light

sulfide sulfur isotopes and the lack of pyrrhotite in the deposit suggest an oxidized

rather than reduced ore-forming environment, it is unlikely that these types of reactions

led to the presence of methane at New Celebration. Phase separation (Naden and

Shepherd, 1989) and post-entrapment hydrogen diffusion (Hall and Bodnar, 1990;

Ridley and Hagemann, 1996) can also account for methane-rich inclusions. At New

Celebration, phase separation of the gold-bearing fluids did not occur until late in the

fault zone evolution, thereby precluding it as a possible source of the pre-gold methane

inclusions. Post-entrapment changes to CO2-CH4 fluid inclusions should result in highly

variable methane contents of individual inclusions within any given cluster or trail,

(Hall and Bodnar, 1990) as not all inclusions would be modified to the same degree.

Laser Raman analyses demonstrate that this is not the case at New Celebration (see

Table 4.1, Chapter 4, Appendix 5), and that the methane inclusions display remarkable

homogeneity. This implies a primary methane dominated source for these fluids. Duan

(1992) determined that fluids above 400 °C could transport significant volumes of CH4

in solution, which suggests that methane-bearing fluids could have a deep crustal or

even mantle source (Polito et al., 2001). This is consistent with the observations of

Kendrick et al. (2008), who, using noble gas analyses of CH4 fluid inclusions at St Ives,


118

determined that methane inclusions from pyrrhotite-bearing quartz veins had argon

ratios and concentrations consistent with a mantle input. In the absence of evidence for

any other mechanism by which methane could have formed at New Celebration, and the

deep crustal and potentially mantle-tapping nature of the BLFZ, the mantle is

considered the most likely origin for methane-bearing fluids at New Celebration.

Highly saline (18-24 wt.% NaCl equiv.) aqueous fluid inclusions, such as those

observed at New Celebration have also been reported from other orogenic lode gold

deposits, however, the origin of these fluids in orogenic lode-gold deposits is

contentious. Unlike some deposits where highly saline aqueous inclusions are

potentially coeval with mineralization-related aqueous-carbonic fluids and likely are the

result of phase immiscibility (Val d'Or, Kerrich and King, 1993) the late highly saline

inclusions recorded in this study only form secondary trails that crosscut and thus post-

date all other inclusion trails and clusters (see Chapter 4) and are therefore

unequivocally post-mineralization. Previous authors (e.g. Boullier et al., 1998) have

suggested that secondary saline inclusions observed in other orogenic lode gold deposits

are crustal shield brines, however, K/Ca ratios >1, derived from LA-ICP-MS analyses

of these inclusions at New Celebration (Table 4.2, Chapter 4) show that these fluids are

likely compatible with magmatic fluids (cf. Yardley, 2005 and references therein)

associated with granitic intrusions late in the evolution of the orogen (cf. Champion and

Sheraton, 1997).

6.4.3 Cation Ratios and Metal Concentrations in Hydrothermal Fluids

There are few published data of metal concentrations in hydrothermal fluids

from orogenic lode gold deposits, and the majority of those published present bulk

crush-leach analytical techniques. Diamond (1990) and Yardley (1993) examined the

fluid characteristics of metamorphic gold-quartz veins from Brusson in NW Italy and

Pike (1993) studied low-salinity, gas-rich fluids in pegmatites from the Muiane deposit,

Mozambique. More recently Olivo et al. (2006) employed single inclusion laser

ablation-time of flight-inductively coupled plasma-mass spectrometry (LA-TOF-ICP-

MS), in conjunction with crush-leach and microthermometry, to evaluate the fluid

compositions in barren and gold-bearing veins from the Sigma deposit in Canada. None

of these studies presented gold data. Relative to aqueous-carbonic fluids from Muiane

or Brusson, K, Mg, Cu, Mn and Fe concentrations in gold-related aqueous carbonic

fluid inclusions at New Celebration are elevated, whereas Na concentrations are lower.


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Minor element/Na ratios of New Celebration fluids are generally an order of magnitude

lower than those from the Sigma deposit, with the exception of As, which is higher at

New Celebration.

More single inclusion data are available from porphyry systems, generally

because fluid salinities are higher and elemental concentrations are determined for each

individual inclusion based on their ratio to Na. Small or dilute inclusions that contain

Na near or below the detection limit will have poor accuracy and precision, something

that hampered individual inclusion analysis in the small, dilute fluid inclusions

characteristic of orogenic lode gold deposits prior to the development of new

technologies used to analyze the New Celebration fluid inclusions. Despite new

advances in technology, which have allowed for smaller beam diameters and analyses

that are more sensitive, there is still a significant dearth of in situ Au analyses. Fluids

from the Butte porphyry system (Rusk et al., 2004), contain Na, K, Pb, Zn and Mn in

similar concentrations to gold-related fluids from New Celebration. Ulrich et al. (1999)

published Au concentrations averaging up to 10 ppm in vapor inclusions from the

Grasberg porphyry Cu-Mo-Au deposit, however, these Au concentrations were

analyzed from high-salinity inclusions.

The post-gold hydrothermal fluids at New Celebration are low temperature, high

salinity fluids with a Na>K>>Mg signature. When comparing these fluids

characteristics with Canadian shield brines, sedimentary basin, metamorphic, and

geothermal fluids (Yardley, 2005 and references therein), it is evident that the shield

brines and basin fluids show no similarities to the New Celebration post-gold fluids.

The metamorphic, geothermal and magmatic fluids, however, exhibit a number of

similarities; Na, K and Mg concentrations are comparable in all fluid types, whereas Ca

and Cu concentrations in the New Celebration fluids are most similar to magmatic

fluids. Lead and Zn concentrations are more closely aligned with metamorphic or

geothermal fluids.

As with many orogenic lode gold deposits around the world, the source of the

hydrothermal fluids and metals at New Celebration remain unconstrained. Potassium,

Mg and Ca over Na ratios, and high base metal concentrations in Stage II related fluids

relative to Stage I indicate that at least two different gold-bearing fluids were

responsible for gold mineralization at New Celebration at different times. The origins of

these fluids are likely metamorphic or magmatic (Ridley and Diamond, 2000), or a


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combination of the two, and maybe locally or regionally derived, however their exact

sources are equivocal.

The presence of Cu, Pb and Zn in the ore fluids and the corresponding lack of

base metal sulfides in the New Celebration gold deposits require an explanation.

Analytical error can be discounted as daily calibration using NIST and in-house

standards assured that precision and accuracy of the analyses were within acceptable

limits. In order to ensure that the results represented the fluid inclusion contents and not

host vein mineral concentrations, only spectra with coincident Na and other cation

peaks were processed. Inclusion-free quartz was check analyzed for interference and

produced no signal.

Significant amounts of base metals do not typically characterize orogenic lode

gold deposits (Kerrich and Hodder, 1982; Hagemann and Cassidy, 2000), and the

geochemistry of base metal-bisulfide complexes is poorly understood (Wood and

Samson, 1998); however, recent advances in single-inclusion laser-ablation inductively

coupled plasma mass spectrometry have allowed detailed investigations of ore fluid

compositions. Olivo et al. (2006) reported Cu/Na, Pb/Na and Zn/Na ratios up to an

order of magnitude higher than those reported in this study, without any associated base

metal mineralization. This would suggest that base metals in lode gold fluids maybe

more common than previously anticipated. The lack of significant base metal sulfides in

orogenic lode gold deposits therefore, suggests either that the physico-chemical

conditions for the precipitation of base metals are not favorable, or that they precipitated

elsewhere in the hydrothermal system.

Base metals are transported as bisulfide or chloride complexes and precipitate

due to changing pH and cooling (Reed, 1998). In orogenic lode gold deposits at mid-

crustal levels, such as the New Celebration gold deposit, wall rock assemblages buffer

ore-fluid pH to near-neutral or slightly alkaline values, and high fluid-rock ratios ensure

that fluid compositions remain constant (Mikucki, 1998). Phase separation can increase

fluid pH as acidic volatiles such as H2S, CO2 and SO2 partition into the vapor phase

(Drummond and Ohmoto, 1985; Naden and Shepherd, 1989; Mikucki and Groves,

1990; Bowers, 1991), however, except in Stage II, Fracture style, phase separation was

not significant at New Celebration. There is also no evidence for either K or CO2

metasomatism, both of which promote gold mineralization by reducing fluid pH, and

the lack of H2 detected in the ore fluids by laser Raman methods indicate that there was

no variability in fluid pH. The lack of distinct cooling and pH changes at New


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Celebration suggests unfavorable conditions for base metal precipitation. It is, therefore,

most likely that the reason for the absence of base metals at New Celebration is that

base metals did not precipitate out of solution but instead discharged through the

outflow zone of the hydrothermal system. If base metal sulfides were precipitated at

New Celebration, they either formed above the current level of the gold deposit and

were exposed and eroded during uplift, or precipitated below the deposit and have not

been intersected by deep diamond drilling, which currently penetrates about 250m

below the pit floor. According to Reed (1998) in high sulfidation epithermal gold

systems that undergo boiling, base metal sulfides will precipitate prior to gold

formation. However, given that the New Celebration gold deposit does not show any

characteristics of an epithermal deposit, and that a boiling horizon has not been

identified, this possibility remains highly unlikely. Further single inclusion laser

ablation –ICP-MS analyses of lode gold hydrothermal fluids from other deposits may

indicate whether base metals are a characteristic of orogenic lode gold deposits, or

whether they are unique to New Celebration only.

6.4.4 Sulfur Isotopes

McCuaig and Kerrich (1998) considered that most Archean orogenic gold

deposits worldwide had sulfide sulfur isotopic compositions between 0 and 9 per mil,

and that this indicated a uniform fluid sulfur source with an isotopic composition

between -1 and +8 ‰ and a fluid redox state below the H2S-SO2 boundary. More

recently, Hodkiewicz et al. (2009) compiled sulfide sulfur isotopic data from orogenic

gold deposits of the Eastern Goldfields Province and reported a range of values between

-10.2 per mil and + 12.7 per mil, with average mean values between -4.0 per mil and

+4.0 per mil. There are a number of deposits both in Australia and around the world,

including the New Celebration deposit, which contain ore-stage pyrites with sulfur

isotopic signatures that are systematically depleted relative to the mostly uniform -1 to

+8 per mil values referenced by McCuaig and Kerrich (1998) and consequently there

are a range of hypotheses proposed to explain these negative values.

Results of some North American studies (e.g. Goldfarb et al., 1991; Thode et al.,

1991) have indicated that the composition of pyrites in some deposits with

systematically 34S enriched or depleted sulfides correlate with the composition of their

host sediments. Sulfides from vein deposits within the orogenic mesothermal Juneau

gold belt in Alaska have significantly depleted and widely variable 34S values relative

to other deposits, with compositions ranging between -17.8 and +1.2‰. Goldfarb et al.


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(1991) attributed the depleted sulfide values to local contributions of sulfur to the ore

fluid at the depositional site. At the Hemlo deposit in Ontario, Canada, Thode et al.

(1991) concluded that the depleted 34S values and wide range of values (-15.9 to +1‰)

observed in gold-related pyrites resulted from fluid-rock reactions and isotopic

exchange between hydrothermal pyrite and sedimentary barite in the host rocks.,

The Fimiston and Oroya lodes of the giant Golden Mile deposit have negative

mean values and broad intra-deposit ranges, up to 22 per mil from Fimiston Lode

mineralization (Hagemann et al., 1999; Bateman and Hagemann, 2004). Hagemann et

al. (1999) and Bateman and Hagemann (2004) concluded that the depleted values and

extreme range in 34S recorded at the Golden Mile resulted from a combination of

diverse mineralization processes, such as phase immiscibility and fluid mixing, and

multiple (igneous, sedimentary, seawater) fluid sources.

In a detailed study of eight vein and shear-hosted orogenic lode gold deposits of

the EGP, including New Celebration, Hodkiewicz (2003) and Hodkiewicz et al. (2009)

indicated that structural style was the most important factor controlling the distribution

of 34S(py) values. In their regional study, Hodkiewicz et al. (2009) concluded that

fault-induced phase separation in gently dipping dilational structures would lead to fluid

oxidation, and that mixing of these modified fluids with original unmodified fluids

would lead to negative 34S(py) values and extreme ranges of values without invoking

the need for magmatic fluid sources or meteoric water contributions. At New

Celebration, which is hosted in a steeply dipping compressional structure, they

established a negative correlation (r2=0.73, n=5) between whole rock gold values and

the sulfur isotopic composition of pyrite to propose that the negative isotopic

compositions of pyrite resulted from in situ oxidation of the ore fluid by carbonation

reactions with pre-existing magnetite and hematite.

Mikucki (2000, 2001, unpublished AMIRA reports), demonstrated that the

magnetite carbonation model for in situ fluid oxidation was not viable at high fluid-rock

ratios except where CO2-CH4 exchange was chemically inhibited. Further, this study

revealed no such correlation between gold grade and 34S values (r2=0.10, n=28), and

that there was no petrographic evidence for carbonation of Fe-oxides. The strong

positive correlation between pyrite abundance and gold grade indicates that wall rock

sulfidation reactions between gold-bearing hydrothermal fluids and host rock Fe-oxides

was the major factor in focusing gold mineralization at New Celebration. Given that

neither carbonation nor sulfidation of wall rock magnetite will lead to in situ oxidation


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of the mineralizing fluid (Mikucki, 2000; Palin and Xu, 2000; Mikucki, 2001), the

depleted sulfur isotopic composition of ore-stage pyrite at New Celebration, therefore,

reflects either the initial composition of the sulfur (Stage I Mylonite and Porphyry-style

and Stage II Contact-style) or oxidation of the ore fluid by phase separation (Fracture-

style Stage II).

6.4.5 Structural Setting

The relationship between Archean orogenic lode gold deposits and first-order

crustal scale fault systems is well established (Eisenlohr et al., 1989; Neumayr et al.,

2000), but these faults themselves do not, for the most part, host the ore deposits.

Rather, at camp- to deposit- scale, distinct second- and higher-order splays branching

off the major crustal-scale structures host the majority of world class (>100t Au)

orogenic lode gold deposits (Eisenlohr et al., 1989; Groves, 1990). An exception to this

is the first-order Larder Lake-Cadillac deformation zone in the southern Abitibi belt of

Canada, which hosts the world-class Kerr-Addison-Chesterville lode gold deposit, in

addition to a number of other deposits and known gold occurrences (Channer and

Spooner, 1991; Smith et al., 1993). Limited research on other major crustal fault zones

around the world, however, indicate that these structures are, for the most part, barren

(e.g. Neumayr and Hagemann, 2002). The Bardoc Tectonic Zone (BTZ) to the north of

Kalgoorlie in the Eastern Goldfields Province is linked to the BLFZ and hosts a number

of small gold deposits and occurrences, however gold production from the BTZ is an

order of magnitude lower than that of the BLFZ (Morey et al., 2007). Morey et al.

(2007) considered that the lack of gold endowment of the BTZ was due to its structural

simplicity, i.e., no secondary splays or large scale antiforms, and its attenuated

deformation history relative to the BLFZ.

6.5 Key factors in the Location of the New Celebration

Deposit

In contrast to most other crustal scale fault systems around the world, the BLFZ

is unique in that it hosts the New Celebration gold deposit within the first-order segment

of the fault and not within adjacent higher-order splays. The key factors in the location

of the New Celebration deposits within the BLFZ appear to be: (1) the long-lived and

complex deformation history of the fault starting with the development of the fault as

discrete N-S-striking steeply dipping thrust faults during D2 compression, followed by

at least two periods of reactivation during D3 and D4; (2) its exposure to a number of


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different fluids such as possible mantle sourced methane, aqueous-carbonic fluids from

two chemically differing crustal reservoirs, and high-salinity aqueous fluids possibility

reflecting magmatic or hydrothermal fluids; and (3) lithological complexity resulting

from the intrusion of brittle, felsic porphyry intrusive rocks into ductile deformed mafic

and intermediate rocks along the BLFZ, which provided appropriate chemical (Stage I

and II) and rheological (Stage II) conditions favorable for gold mineralization. The fluid

inclusion record at New Celebration indicates that fluid flow through the BLFZ

continued over an extended length of time during a number of deformation events and

included several chemically different fluids of potentially diverse origins, at least two of

which contained gold and other metals and contributed to gold mineralization at New

Celebration

The presence of iron-rich mafic host rocks and the pre-mineralization

metamorphic magnetite alteration of otherwise chemically unfavorable iron-poor

intermediate host rocks (cf. Groves, 1990; Hodgson, 1993) significantly enhanced the

potential for the BLFZ to host gold mineralization at New Celebration. There is

abundant evidence for magnetite replacement by ore-stage pyrite, which indicates that

sulfidation of the wall rock by the ore-fluid was the most important gold mineralizing

process during Stage I and that the metamorphic magnetite was critical to the formation

of Stage I gold.

Dilation of the shear zone and an anti-clockwise change in the orientation of the

shear zone away from the average trend of the BLFZ (Hodkiewicz, 2003) during late

D3NC and early D4NC provided space for the emplacement of the M2 porphyry into the

fault, which in turn likely facilitated increased fluid flow up the contacts of the

porphyry. The high stress regime within the shear zone resulted in extensive brittle

fracturing of the felsic porphyry (Norris, 1990), during late D3NC and D4NC relative to

other less competent units, and gold mineralization occurred, in part, through failure-

induced pressure reduction and consequent phase separation (Cox et al., 1995; Sibson,

2004). The emplacement of the M2 quartz-feldspar porphyry within the BLFZ was,

therefore, likely a key factor by firstly, focusing the ore-fluid along the high-Mg basalt

contact, which induced Contact-style mineralization, and secondly, by providing a

brittle host, which fractured instead of undergoing ductile deformation during fault

movement, for Fracture-style mineralization. Intrusion of the M2 porphyry may also

have coincided with an influx of a second gold-bearing fluid, possibly of magmatic

origin, into the shear zone.


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6.6 Outstanding Questions

6.6.1 Fluid and Metal Source

The source of hydrothermal fluids and metals remains one of the most

contentious and divisive issues facing researchers and explorers studying and exploring

for orogenic lode gold deposits around the world. This study determined that the

mineralizing events at New Celebration were the result of two distinct fluids circulating

through the BLFZ at separate times and in different hydrothermal P-T regimes. Cation

ratios and base metal concentrations of hydrothermal ore fluids indicate that a switch in

fluid source took place between Stage I and Stage II, and K/Ca ratios indicate that the

Stage II New Celebration fluids have closer affinities to magmatic fluids than to

metamorphic (see Table 4.2, Chapter 4). Sulfur isotopic compositions of ore-stage

pyrite, even though unable to demonstrate unequivocally the source of the ore fluids,

indicate that they are more oxidized than those encountered in most orogenic lode gold

deposits, and as such, may reflect contributions from oxidized granitic sources. Trace

element geochemistry of oxides and ore-stage sulfides support the conclusions that

Stage I and Stage II formed from chemically distinct ore fluids and from different ore

forming processes.

Advances in new techniques such as noble gas (He, Ne, Ar, Kr, Xe), and

halogen (Br, Cl, I) analyses of well constrained methane and aqueous-carbonic fluid

inclusions, in addition to existing techniques such as carbon isotopic analyses on

methane and carbonic inclusions, as well as nitrogen isotopic analyses of

mineralization-related mica alteration, are allowing new interpretations of genetic

models for orogenic lode gold deposits. Noble gases have well constrained isotopic

compositions that vary by orders of magnitude between the mantle and the crust, they

have low abundances and are inert (Ozima and Posodek, 2002). Their rarity means that

they are transported in volatile phases, such as H2O, CO2 and CH4, which are important

for metal transport. Their isotopic composition provides constraints on, and in some

cases, definitive proof of, mantle fluid involvement in gold mineralization (Simmons et

al., 1987), and concentration modifications that take place during wall rock reactions

and phase separation provide information on ore forming processes (Kendrick et al.,

2001; Kendrick et al., 2006). In their recent study of H2O-CO2 and CH4 fluid inclusions

at St Ives, Kendrick et al. (2008) determined that H2O-CO2 inclusions from oxidized

pyrite-bearing quartz veins had 40Ar/36Ar ratios and Ar concentrations consistent with

magmatic fluids, and that CH4 inclusions from reduced pyrrhotite-bearing quartz veins


126

had argon ratios and concentrations consistent with a mantle input. Carbon isotopic

analysis of carbon in fluid inclusions, which provides direct evidence for the

composition of ore forming fluids, was attempted at New Celebration but was

unsuccessful due to the small size of the fluid inclusions (typically <10 µm) and low

abundance of inclusions in quartz veins.

Recent advances in the analysis of the nitrogen isotopic composition of gold-

related mica mineralization may also help resolve the issue of hydrothermal fluid

source. Ammonium (NH4) substitutes for K in potassium silicate minerals (Honma and

Itihara, 1981) and the 15N composition of various crustal and mantle rocks are well

constrained (Jia and Kerrich, 1999 and references therein). Studies on the nitrogen

isotope systematics of micas in orogenic gold-bearing quartz veins of the North

American Cordillera (Jia et al., 2003), quartz veins systems in the Bendigo Gold Field

of Eastern Australia (Jia et al., 2001) and intrusion-hosted deposits of the Charters

Towers Goldfield, Northern Queensland (Kreuzer, 2005), in conjunction with, C, H and

O isotopes, have provided better constraints on the possible sources (metamorphic,

magmatic, meteoric, mantle of hydrothermal fluids within these systems. The

application of newly developed techniques, such as noble gas, halogen and nitrogen

isotope analyses, to well constrained fluid inclusions, may help clarify the source (or

sources) of hydrothermal fluids in orogenic gold systems.

6.6.2 Timing of mineralization

The absolute timing of gold deposition at New Celebration, and the time gap

between the two mineralizing stages is also unconstrained. Pressure-temperature

estimates of 280-360 °C and 1.0-3.5kbars indicate that Stage II mineralization occurred

after a period of interpreted uplift and erosion (Fig. 4.6, Chapter 4) and during a change

from a ductile to a brittle deformational regime during crustal cooling or increasing

strain rate (Weinberg et al., 2005). However, it is unknown how much time separated

these two events. This could be resolved by U-Pb SHRIMP (sensitive-high resolution

ion microprobe dating of zircons within the host M1 and M2 porphyry dikes or ore-

related hydrothermal monazite, traces of which were observed petrographically and by

using a scanning electron microscope (SEM; Nichols, 2003). The Re/Os dating of ore-

stage pyrite as well as Ar/Ar dating of sericite included in ore-stage pyrite could

potentially constrain mineralization ages (Phillips and Miller, 2006).


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6.7 Summary

The paleohydrothermal evolution of the BLFZ and New Celebration gold

deposits is characterized by discrete pulses of gold-bearing and barren hydrothermal

fluids infiltrating the fault as a consequence of distinct deformation events (D3NC to

D4+NC). At least two gas-rich fluid events are recorded that cannot be conclusively

linked to gold mineralization. These comprise: (1) CH4-dominant fluids, which appear

to span the life of the hydrothermal system, and may be mantle derived, evidenced by

the presence of lamprophyres within the fault at New Celebration, and the lack of

evidence for contributions from carbonaceous country rocks or post-entrapment

modification of H2O-CO2 inclusions; and (2) CO2-dominant fluids, whose petrographic

relationship to the gold related fluids is unclear, but which may represent magmatic

volatiles (cf. Neumayr et al., 2008). The gold mineralization stages are characterized by

low salinity (0.4-7.4 wt. % NaCl equiv.) aqueous-carbonic inclusions (XCO2=0.05-

0.73) with NaCl, KCl, CaCl2 and rare CH4 and as such are similar to many other gold-

bearing fluids observed in many orogenic gold deposits worldwide. There is no fluid

inclusion evidence for significant surface water infiltration into the BLFZ (cf.

Hagemann et al., 1993), and remobilization of gold from carbonaceous sedimentary

rocks (c.f. Large et al., 2009) therefore, the switch in K/Ca ratios may relate to a change

in “deep” fluid sources such as magmatic, metamorphic or mantle fluids. Further

investigations on the gold-bearing and gas rich fluids should include detailed analyses

of the stable (H, C, O, N) and radiogenic (40Ar/36Ar) isotopes, in addition to noble gas

and halogen contents to elucidate further the nature of the “deep” fluid sources.

CHAPTER SEVEN: GOLD MINERALIZATION AND THE BLFZ

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7 CHAPTER SEVEN: PROTRACTED GOLD MINERALIZATION IN THE KALGOORLIE-KAMBALDA CORRIDOR AND ITS RELATIONSHIP TO THE BOULDER-LEFROY FAULT ZONE, EASTERN GOLDFIELDS PROVINCE, WESTERN AUSTRALIA

J.L. Hodge*, S.G. Hagemann, T.C. McCuaig, P. Neumayr

School of Earth and Environment, University of Western Australia, 35 Stirling

Highway, Crawley, WA 6009, Australia

* Corresponding Author: 3502-188 Keefer Place, Vancouver, BC, V6B 0J1, Canada,

[email protected]

This chapter has been prepared for submission as a paper to Ore Geology Reviews and

as such follows the format required by the journal, including American English. The

references are combined with the references from chapters 1-6 and chapter 8, and

presented in a consistent list at the end of the thesis. In situ sulfur isotope and laser

ablation ICP-MS mineral chemistry methodologies are presented as Appendix 10.

Sulfide sulfur isotopic compositions and sulfide, oxide and gold mineral chemistry

analyses are contained in Appendices 7 and 8 of the thesis, respectively. The first author

conducted the laser ablation ICP-MS mineral chemistry analyses and the in situ sulfur

isotopic analyses not specifically referenced to other researchers. The first author also

conducted the literature research and wrote first draft of the paper. Co-authors S.

Hagemann, T.C. McCuaig and P. Neumayr read drafts of this paper and made scientific

and editorial comments.

ABSTRACT

New geochemical data from the giant Golden Mile and world-class New

Celebration and St Ives gold deposits (>2000 t Au total), in conjunction with data

collected during almost 100 years of research on the gold deposits of the Kalgoorlie-

Kambalda corridor, indicate that the Fimiston and Oroya mineralization styles are

unrelated to the crustal-scale Boulder Lefroy Fault Zone (BLFZ), or to other gold

deposits in this corridor. The unique Au, Te, Sb association observed in ore-stage pyrite

in the Fimiston and Oroya lodes, in conjunction with extensive roscoelite alteration and

the abundance and diversity of syn-mineralization telluride minerals suggests a link to

mailto:[email protected]


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alkalic magmatism and emplacement at shallow crustal depths (<6km) at temperatures

below 300° C. Structural evidence indicates that these lodes formed during D1 prior to

the establishment of the BLFZ during the change from extension to compression across

the orogen. Similar ore-stage sulfide trace element chemistry from the New Celebration

and St Ives deposits, and their structural location relative to the BLFZ, indicate that

these deposits formed during the same D3 deformation event, and that the hydrothermal

fluids were sourced from the same crustal fluid reservoirs. At the Golden Mile,

underlying rift architecture likely facilitated the movement of gold-rich fluids to the

upper crust where ideal physico-chemical conditions resulted in the formation of the

richest square mile of gold on earth.

1. INTRODUCTION

The Boulder Lefroy Fault Zone (BLFZ), which is located in the central portion

of the 60 km long by 15 km wide Kalgoorlie-Kambalda corridor, is spatially related to

one giant (> 1000t Au), two world-class (>100 t Au) and numerous smaller gold

deposits which together have produced about 2000 tonnes of gold in the last 110 years.

This makes the BLFZ likely the richest gold-endowed fault system on earth.

Researchers have been studying the various gold deposits within this corridor almost

since the initial discovery of gold in Kalgoorlie in 1893; however, no project has drawn

together the abundant available structural, mineralogical and geochemical data to

evaluate the exact role of the BLFZ with respect to the location of gold mineralization

within the Kalgoorlie-Kambalda corridor. This study presents a synthesis of the

existing, and new geological data (Mueller, 2007; Miller et al., 2009; Hodge et al., in

revision), to evaluate the potential role of the BLFZ in forming the giant and world-

class deposits that make the Kalgoorlie-Kambalda corridor so unique.

In the Eastern Goldfields province of Western Australia, the conventional model

for gold mineralization in the Kalgoorlie Terrane is that the bulk of Au mineralization

was introduced during mid- to late regional D3 metamorphism at approximately 2630

Ma (Kent and McDougall, 1995) and is genetically associated with the activation and

reactivation of the Boulder Lefroy Fault Zone (e.g. Clark et al., 1986; Norris, 1990;

Phillips et al., 1996; Nguyen, 1997; Copeland, 1998; Weinberg et al., 2005)

Recent work on the Golden Mile, however, has highlighted discrepancies in the

traditionally accepted syn-D3 mineralization age, and suggests that gold mineralization

episodes, at least at Kalgoorlie, occurred over a far more protracted time period,


130

possibly as long as 50 Ma (Bateman et al., 2001; Bateman and Hagemann, 2004;

Gauthier et al., 2004; Gauthier et al., in revision). New fluid inclusion data from the

New Celebration deposit, indicate a more complex fluid history at the New Celebration

deposit in the BLFZ, (Hodge et al., in revision), than previously postulated, and recent

investigations at the St Ives camp indicate a far more protracted structural and

hydrothermal history associated with gold mineralization (Neumayr et al., 2008; Miller

et al., 2009) than traditional models postulate. In conjunction with new mineral

chemistry data obtained during this study, these findings suggest that the structural and

hydrothermal history of the BLFZ is more complicated than previous models suggest.

This has highlighted the need for an integrated appraisal of regional scale structural and

hydrothermal fluid systems operating during the Archean.

The Golden Mile, New Celebration and St Ives deposits were chosen to evaluate

similarities and differences in ore mineralogy, alteration systematics and fluid chemistry

for three reasons: (1) they are giant (Golden Mile) and world-class (New Celebration, St

Ives) deposits, which have been studied in detail; (2) both deposits, in addition to New

Celebration, are spatially (and genetically?) related to the crustal-scale BLFZ (Fig. 1);

and (3) well-constrained sample material was readily accessible. Samples for sulfur

isotopic and LA-ICP-MS mineral chemistry analyses from the Golden Mile were

chosen to characterize the different mineralization styles (Fimiston and Oroya),

different lode systems (East and West), different chronological events within a single

lode system (Fimiston Stages I-IV), and shallow versus deep (>600 m below current

surface) gold mineralization (Hagemann et al., 1999). The New Celebration samples

were chosen to represent early and late gold mineralization stages (Hodge et al., in

revision; Nichols et al., in revision), and the St Ives samples were chosen to represent

reduced, pre-gold hydrothermal assemblages, oxidized main-stage gold-related

assemblages and late gold-related hydrothermal assemblages described by Petersen et

al. (2006) and Neumayr et al. (2008).

This paper presents a review of existing structural, hydrothermal alteration,

mineralogical and geochemical from the Golden Mile, New Celebration and St Ives

gold deposits, with new data on the sulfur isotopic composition and mineral chemistry

of hydrothermal oxides, ore-stage pyrites and gold, and integrates the data into a

regional-scale hydrothermal evolution model for the Kalgoorlie-Kambalda corridor.


131

2. REGIONAL GEOLOGY

The late Archean Eastern Goldfields Province (EGP, Fig. 7.1) is located at the

eastern margin of the Yilgarn craton. The Kalgoorlie Terrane (Fig. 7.1) is a 6 to 9

kilometer thick, elongate, NNW trending volcano-sedimentary sequence which is

bounded to the east and west by wide (up to 1km) anastamosing shear zones (Swager,

1997). The volcano-sedimentary greenstone sequence, which correlates across the

terrane (Table 7.1), comprises basalt, komatiite and felsic volcanic and volcaniclastic

rocks, as well as a number of different granitoid suites. Coarse clastic basins, which

unconformably overlie the greenstone sequence, commonly bury major boundary faults

and are the youngest rocks (Swager, 1997). Regionally, the terrane is metamorphosed to

upper greenschist facies, with locally higher metamorphic grades (up to amphibolite

facies) recorded along the margins of, and adjacent to, granitoid plutons (Witt, 1991;

Mikucki and Ridley, 1993). Swager and Nelson (1997) recognized four main

compressive deformation episodes (D1-D4, Table 7.2) in the Kalgoorlie Terrane, each

preceded by extensional periods. The earliest extensional phase was accompanied by the

emplacement of the mafic-ultramafic volcanic succession, (Williams and Currie, 1993;

Passchier, 1994), which was accompanied by widespread hydrothermal sea floor

alteration (Golding et al., 1987; Clout, 1989) and the formation of the Black Flag

Group, during bimodal mafic-felsic volcanism. This was followed by D1 (> 2675 Ma),

which in Kambalda is interpreted to be a period of south over north compression that

resulted in widespread structural repetition and thrust faulting (Swager and Nelson,

1997). In Kalgoorlie, Swager (1995) and Bateman and Hagemann (2004) interpreted D1

as an east-west compressive event, represented by the Golden Mile


132

Figure 7.1 Geological map of the Yilgarn Craton showing the Eastern Goldfields Province, the location of

major gold camps and deposits, the location of the New Celebration, Golden Mile (Kalgoorlie) and St

Ives (Kambalda) gold camps, and the terranes of the Eastern Goldfields Province. Modified from

Bateman and Hagemann (2004). K = Kalgoorlie Terrane, U = Kurnalpi Terrane, G = Gindalbie Terrane,

E = Edjudina Terrane, L = Laverton Terrane, N = Norseman Terrane, BLFZ = Boulder Lefroy Fault

Zone.

Fault. A second extensional phase followed and was accompanied by the formation of

coarse clastic basin sequences (e.g., the Merougil Conglomerate and Kurrawang

Formation) and widespread granitoid intrusion (Weinberg et al., 2003). Regional D2


133

shortening at around 2675-2657 Ma (Nelson, 1997) was approximately east-west and

resulted in north-northwest-south-southeast trending upright folds and penetrative

foliation (Swager, 1989; Swager and Griffin, 1990; Weinberg et al., 2003). During D3

(2663-2645 Ma) and D4 (<2640 Ma) (Nelson, 1997; Swager, 1997), deformation

became strike-slip in nature and progressed from a ductile to a brittle regime (Mueller et

al., 1988; Bateman et al., 2001).

Table 7.1 Correlation between the stratigraphy of the Golden Mile, New Celebration and St Ives gold

camps

Golden Mile (Swager, 1989, Swager et al. 1995) New Celebration (Langsford, 1989) St Ives (Watchorn, 1998)

Kurrawang Formation: Alluvial, fluviatile and shallow-marine coarse clastic sandstone deposited within locally fault-bounded synclines parallel to regional tectonic trend

Merougal Conglomerate Merougal Conglomerate

Black Flag Group: Felsic volcanic and volcaniclastic sedimentary sequence, >1km thick, coarsening upwards

Black Flag Group Black Flag Group

Golden Mile Dolerite: Differentiated tholeiitic dolerite, divided into 10 petrographic units, 800m thick

Triumph Gabbro Condensor and Junction Dolerites

Kalgoorlie Group Paringa Basalt: Up to 1500m thick, high Mg, variolitic, pillowed, cherty interflow sediments

Kyarra Basalt Paringa Basalt

Williamstown Dolerite: Up to 300m thick, fractionated

Pernatty Dolerite, 300-500m thick, basal cumulate pyroxenite

Defiance Dolerite

Kapai Slate: Marker horizon, 5-25m thick, pyritic graphitic slate to magnetite-bearing chert

Kapai Slate Kapai Slate

Devon Consols Basalt: 60-100m thick, high Mg variolitic basalt

Mutooroo Basalt, 100-200m thick Devon Consols Basalt

Hannan's Lake Serpentinite: 800-1200m thick, serpentinized ultramafic lavas grading upward to high Mg basalt

Kambalda Komatiite Kambalda Komatiite

Lunnon Basalt: >200m thick, pillowed tholeiites with thin interflow sediments


134

Table 7.2 Regional deformation of the Kalgoorlie terrane and correlated events reported from the Golden Mile, New Celebration and St Ives gold camps

Age Regional Deformation Golden Mile Gold Camp (Bateman and Hagemann, 2004)

New Celebration Gold Camp (Nichols, 2003)

St Ives Gold Camp (Archibald, 1985; Swager, 1989; Nguyen, 1997

<2640 (Swager, 1997)

D4 dextral shear on NNE-SSW trending shear zones

D4 Right lateral oblique-slip movement on NNE striking faults

D4NC Strike slip movement on the BLFZ. Movement sense unconstrained

D4 NE-SW shortening. Reactivation of pre-existing faults and development of brittle NE and NW faults

2663-2645 (Nelson, 1997; Swager, 1997)

D3 Strike-slip shear with dextral and sinistral movement

D3 Broad scale left lateral transpression resulting in sinistral strike-slip movement on the BLFZ and BS and local scale antithetic right lateral strike slip movement on NNE striking, steeply NW dipping faults

D3NC Sinistral oblique-slip west block down to the SW movement on the BLFZ

D3 ESE-WNW shortening. Sinistral movement on N-trending faults, tightening of D2 folds, reactivation of D2 faults and development of new faults subsidiary to D2 faults

2675-2657 (Nelson, 1997)

D2 ENE-WSW regional shortening, upright foliation and folds (Swager, 1997; Witt and Swager, 1989; Nelson, 1997; Ridley and Mengler, 2000)

D2 NE-SW compression. Development of NNW striking thrust faults, upright folds and NS striking, subvertical axial planar cleavage

D2NC Tilting of conformable subunits of the Pernatty dolerite to vertical orientations

D2 ENE-WSW shortening,. Development of open upright folds such as the Kambalda Dome, and development of main upright (S2) foliation

>2675 (Swager 1997)

D1 Low angle shears, thrusting, stratigraphic repetition, recumbent folds (Swager, 1989; Passchier, 1994, 1995; Swager and Nelson 1997)

D1 (local)

NE-SW compression. Development of N-trending, NE over SW thrust faults and Kalgoorlie Anticline

D1 N-S compression. Development of E-W-trending thrust faults and recumbent folds such as the Foster, Tramways and Republican thrusts.


135

2.1 The Boulder-Lefroy Fault Zone The BLFZ occupies the hinge of a regional D2 anticlinal structure (Swager,

1989) and has a complicated history. There are a number of different interpretations

regarding its movement sense and evolution through time (Fig. 7.3). Swager (1989)

described it as a major oblique sinistral wrench structure, active during D3, based on

asymmetrical relationships with several regional fold structures and segmentation of the

Stony Hill-Mt Goddard Dolerite into strike-slip duplexes. While most authors agree that

the major period of fault formation and movement took place during D3, various

movement senses have been interpreted including reverse movement based on seismic

data (Goleby et al., 2000) and field observations (Boulter et al., 1987; Copeland, 1998;

Ridley and Mengler, 2000), oblique-sinistral movement (Swager, 1989; Witt, 1991;

Nguyen et al., 1998; Nichols, 2003) and dextral movement. Mueller et al. (1988)

described two stages of wrench faulting on the BLFZ; an early phase of sinistral

transpressional shearing during D2 followed by a later phase of dextral transcurrent

shearing, with a thrust component, during D3. Weinberg et al. (2005) also described a

two-stage process for the formation of the BLFZ. However, in their interpretation,

isolated north-south trending thrust ramps, which formed during D2 ~east-west

compression, coalesced into a single cohesive fault zone during sinistral strike-slip

reactivation during D3. Nichols (2003) described D3 sinistral oblique-slip and post-D3

horizontal strike-slip movement of unknown direction on the fault from the New

Celebration open pits where the western segment of the BLFZ is exposed. There are a

number of reasons for the discrepancies between authors when describing the kinematic

history of the BLFZ. For example, the fault has a strike length extending over 200 km,

and in places the fault trace is poorly defined due to limited exposure and extensive

transported cover. Outcrop is generally poor throughout the Kalgoorlie-Kambalda

corridor and there are only limited exposures where observations can be taken directly

from within the fault.

3. HISTORY OF GOLD MINERALIZATION IN THE KALGOORLIE-

KAMBALDA CORRIDOR

Prospectors first discovered gold in Kalgoorlie in 1893 and since then the region

has been in continuous production. Much of the gold mineralization is classified as

orogenic


136

Figure 7.2 Correlation between regional deformation events and gold mineralization and those reported

from the Golden Mile, New Celebration and St Ives camps. From Weinberg et al. (2005).

lode gold, and accounts for most of the gold production in the region. For the first 96

years of production, a number of companies mined the deposit from small pits and

underground

operations. In 1989, these were all combined into a single resource under the

management of Kalgoorlie Consolidated Gold Mines (KCGM), a joint venture between

Newmont Australia and Barrick Gold Corporation. The orogenic gold camp is one of

the largest in the world and has produced over 1,500 tonnes of gold since 1893

(Bateman and Hagemann, 2004).

Gold was initially discovered in the New Celebration area in the 1890’s

(Gresham, 1991), however, mining of any significance did not take place until after

World War I, when the Celebration, Dawns Hope and White Hope mines were

discovered. Rising production costs in the late 1920’s put an end to gold mining in the

area, and exploration did not recommence until the early 1980’s, when the Hampton

Boulder and Jubilee deposits (now comprising the single New Celebration open pit


137

deposit) were discovered (Copeland, 1998). The New Celebration deposit has produced

over 100 tonnes of gold in the modern mining era (Norris, 1990; Copeland, 1998).

Minor copper-gold mineralization (0.257 Mt at 5 g/t Au for 41,300 ounces) is

also located 10 km to the south of the Golden Mile, at the Hannan South and Shea

deposits (Schiller and Ivey, 1990). These deposits are described as Cu-Au oxidized

epidote endoskarns by Mueller (2007) and are associated with calc-alkaline

monzodiorite and tonalite intrusions adjacent to the BLFZ.

Prospectors discovered gold at Red Hill in Kambalda in 1897. Production

continued for 10 years, then recommenced again in 1919 for another 7 years. The region

was largely ignored until the late 1970’s, when an increasing gold price spurred on

renewed exploration efforts. Gold production recommenced in 1981 (Gresham, 1991)

and has continued to the present day . As of January 2007, the Kambalda gold camp had

produced over 265 tonnes of gold (Neumayr et al., 2008).

4. GEOLOGY OF THE MAJOR GOLD CAMPS IN THE KALGOORLIE-

KAMBALDA CORRIDOR

4.1 Deposit Geology 4.1.1 Golden Mile

The giant Golden Mile camp comprises a number of deposits that in 1989 were

combined under the ownership of Kalgoorlie Consolidated Gold Mines (KCGM) to

form the single Golden Mile deposit (Fig. 7.4). The deposit comprises three major styles

of gold mineralization: the Fimiston and Oroya gold-telluride lodes, which together

have produced the majority of the gold from the Golden Mile, and the Mt Charlotte gold

lodes. All gold mineralization styles are predominantly hosted within the Golden Mile

Dolerite, a 700m thick differentiated tholeiitic sill that intruded the contact between

Paringa Basalt and overlying Black Flag Group metasedimentary rocks. Fimiston

mineralization, forms narrow (<2m) laterally and vertically extensive lodes (Gauthier et

al., in revision) that, are separated into Eastern and Western Lodes by the D1 Golden

Mile fault. Open space fill textures, such as comb, cockade, crack-seal and banded veins

characterize Fimiston-style mineralization. Oroya lodes, which are defined by their high

abundance of telluride minerals and “green leader” V-rich mica alteration (Larcombe,

1912), crosscut Fimiston lodes (Bateman et al., 2001; Bateman and Hagemann, 2004).

Mt Charlotte style


138

Figure 7.3 Geology of the Golden Mile camp (Bateman and Hagemann, 2004

sheeted quartz-carbonate±scheelite mineralization locally overprints all other lodes at

the Golden Mile, and formed predominantly within unit 8 of the Golden Mile Dolerite.

The Mt Charlotte deposit is the type locality for this mineralization style, however,

Charlotte-type mineralization is observed throughout the Golden Mile. In all

mineralization styles at the Golden Mile, wall-rock reaction of sulfur- and gold-bearing

hydrothermal fluids with iron-rich wall rocks precipitated gold however, phase

separation was locally important, and the high quartz content of unit 8 in the Golden

Mile Dolerite, which imparted a significant competency contrast between it and

surrounding country rocks, was fundamental in the location of the Mt Charlotte

stockwork veins (Bateman et al., 2001; Bateman and Hagemann, 2004).

4.1.2 New Celebration

The New Celebration gold camp comprises six open pits (Hampton-Boulder,

Jubilee, Mutooroo, Celebration, Golden Hope and Early Bird) and four underground ore

zones within the Hampton Decline operation. The Hampton-Boulder and Jubilee open

pits, which until 2001 were separately owned, were amalgamated into a single resource

now referred to as the New Celebration deposit. Gold mineralization at the New

Celebration deposit is hosted within the Boulder Lefroy Fault Zone, in the sheared-out

hinge of the Celebration Anticline. Gold mineralization is located in a sequence of

mafic and ultramafic volcanic rocks intruded by a number of felsic and intermediate

porphyry dikes (Fig. 7.5). The mine sequence, from footwall to hanging wall, comprises

serpentine-tremolite-chlorite-talc altered Kambalda Komatiite, high-Mg basalt schist

and a differentiated dolerite unit, which is schistose proximal to the fault. The contacts


139

between the komatiite, high Mg basalt and dolerite are conformable, and are intensely

sheared and hydrothermally altered at the BLFZ (Norris, 1990; Williams, 1994;

Copeland, 1998). Two major porphyry stages intrude this contact along the BLFZ: an

early intermediate porphyry, denoted M1 by Nichols (2003), which is strongly

deformed and biotite-ankerite-albite-sericite altered, and a later feldspar-phyric

porphyry (M2), which is boudinaged along strike and down dip, and attains widths of

up to 80m in places. Ore zones are located in the hanging wall of the contact between

the ultramafic and mafic rocks, and are located within and immediately adjacent to the

M1 and M2 porphyries, which intrude the contact along the BLFZ (Norris, 1990;

Williams, 1994; Copeland, 1998; Nichols, 2003). Deformed and mylonitized M1

intermediate porphyries and mafic schists host Stage I gold mineralization (Nichols,

2003), which formed by sulfidation reactions with metamorphic magnetite (Hodge et

al., in revision). Stage II gold mineralization, which is hosted in M2 porphyry dikes and

the contact between the dikes and high Mg basalt (Nichols, 2003) formed by a

combination of wall rock reaction and phase immiscibility (Hodge et al., in revision)

4.1.3 St Ives

The St Ives gold camp) is the second largest in the Kalgoorlie-Kambalda

corridor after the Golden Mile. It is located approximately 30km south of Kambalda,

and incorporates the Victory, Revenge, Defiance, Britannia, Sirius, Orchin, Thunderer,

Phoebe, Leviathin, Junction and Argo deposits (Fig. 7.6 (Hagemann and Cassidy,

2001). The St Ives gold camp is bounded by the BLFZ to the east and the Zuleika shear

zone to the west, and gold mineralization is dominantly controlled by the Playa shear

zone, interpreted as a second-order splay off the BLFZ (Nguyen et al., 1998; Watchorn,

1998). Mafic (Paringa Basalt, Devon Consols Basalt, Defiance Dolerite), ultramafic

(Tripod Hill Komatiite) interflow sedimentary (Kapai Slate) rocks, and minor felsic

porphyries, all metamorphosed to upper-greenschist and lower amphibolite facies, host

the majority of gold mineralization at St Ives, which is located in quartz breccia zones,

brittle-ductile shear zones and brittle quartz vein arrays (Clark et al., 1986). A number

of mechanisms have been proposed for


140

Figure 7.4 Geology of the New Celebration gold deposit. From Nichols (2003)


141

Figure 7.5 Geology of the St Ives gold camp. From Neumayr et al. (2008)

the formation of gold mineralization at St Ives including sulfidation of iron-rich wall

rocks (Clark et al., 1989), phase separation (Clark et al., 1986), carbonation of wall rock

magnetite (Palin and Xu, 2000) and fluid mixing (Neumayr et al., 2005; Neumayr et al.,

2008).

4.2 Deformation and Timing of Gold Mineralization in the Kalgoorlie-Kambalda Corridor Generally, models of gold mineralization within Archean terranes place the

mineralizing event late in the evolution of the host terrane (Colvine et al., 1988; Groves

et al., 1989; Kerrich and Cassidy, 1994). Within the regional structural framework of

Swager (1989) gold mineralization is interpreted to have taken place over a restricted

time interval, during late D3, post-peak metamorphism, and associated with reactivation

of crustal-scale deformation zones (Groves, 1993). At least one stage of mineralization

at the New Celebration gold camp is also consistent with a syn-late D3 origin. Nichols

(2003) interpreted Stage I gold mineralization as contemporaneous with D3NC

deformation, based on the textural relationships between ore-bearing sulfides,

hydrothermal alteration minerals and D3NC foliations. This interpretation is consistent


142

with the observations of other authors (Witt, 1993b; Copeland, 1998; Weinberg et al.,

2005) who also proposed a D3 origin for gold mineralization at New Celebration.

At St Ives, observations made on a number of different deposits indicate that

gold mineralization formed during D4. Clark et al. (1986) established that auriferous

veins and breccias at the Victory deposit were associated with retrograde carbonation of

peak metamorphic assemblages and constrained mineralization to late in the mine-scale

deformation history. The 40Ar/39Ar dating of metasomatic biotite alteration associated

with gold mineralization initially constrained the minimum age of gold mineralization

to 2601±3 Ma (1) (Clark, 1987), however, recalculation of these data (T.C. McCuaig,

unpublished data) indicated that there was an approximately 1 percent error (26 Ma)

indicating a minimum age of 2627±3 Ma. Nguyen (1998) indicated that mineralization

at Revenge took place late in the tectonic evolution of the camp and obtained a U/Pb

date for gold-related hydrothermal monazite mineralization of 2631±4 Ma. They

considered monazite precipitation synchronous with D3 and interpreted that the gold

mineralization was associated with reverse shear zones formed during D3 oblique-slip

faulting on the BLFZ. Nichols (2003)identified a second, brittle-ductile mineralization

event, at New Celebration, and based on cross-cutting relationships between M1 and

M2 gold-hosting porphyries, interpreted this event as late D3NC or early D4NC

Groves (1993) considered the Fimiston lodes at the Golden Mile to be syn-D3

(2660 to 2632 Ma, Nelson, 1997; Swager et al., 1997), consistent with the crustal

continuum model, whereby gold mineralization occurs over a restricted time period late

in the structural evolution of the host Archean terrane. Recent evidence, however,

indicates that the Fimiston and Oroya lodes are much older. Bateman et al. (2001) and

Bateman and Hagemann (2004) used the relative structural timing of a number of key

structures to constrain Golden Mile mineralization to late D1 early D2. These authors

provided the following evidence for this interpretation: (1) Fimiston lodes are cut by all

structures, including the D1 Golden Mile Fault; (2) the Oroya shoot resides within a

dilational jog between the D2 Oroya hanging wall and footwall shears, which

themselves crosscut the Fimiston lodes; (3) the Adelaide fault, the major regional D3

structure, cuts the Lake View (part of the Fimiston group) lode; and (4) D3 faults have

deformed the lodes consistent with east over west reverse movement. More recently,

Gauthier et al. (in revision) dated an andesite dike suite interpreted as being

contemporaneous with Fimiston lodes at 2663±11 Ma, constraining Fimiston-style

mineralization to the period 2674 to 2652 Ma.


143

Structural evidence indicates that the Mt Charlotte lodes formed during D4

brittle-ductile faulting. The Mt Charlotte quartz veins crosscut, and are crosscut by

brittle-ductile D4 faults, and reactivated D2 faults indicating contemporaneous fault

movement and vein formation during D4. Kent and McDougall (1995) dated

hydrothermal sericite (40Ar/39Ar) from alteration haloes around gold-bearing quartz

veins at 2602±8 Ma (recalculated to 2625 Ma by L. Snee: Bateman et al., 2001), and

Phillips and Miller (2006) calculated an 40Ar/39Ar date of 2594±8 Ma (2) for

muscovite inclusions within pyrite from Mt Charlotte. Bateman et al. (2001) and

Bateman and Hagemann (2004) interpreted all of these data as indicating that gold

mineralization in the Kalgoorlie camp was a protracted event, which took place over a

period of approximately 50 Ma and which formed distinct and diverse mineralization

styles.

4.3 Hydrothermal Alteration Mineralogy Spatially and/or Temporally Related to Gold Mineralization A laterally extensive zone of chlorite-carbonate alteration extending up to 1 km

from the deposit surrounds the Golden Mile, which Phillips (1986) interpreted as gold

mineralization-related. Clout (1989) described three main alteration types associated

with the Fimiston and Oroya lodes: (1) distal ankerite-sericite-quartz-pyrite, containing

0.1 to 3.0 g/t Au; (2) proximal ankerite-siderite-quartz-hematite-pyrite-

tellurides±albite±tourmaline±magnetite, containing up to 50 g/t Au; and (3) “green

leader”(Larcombe, 1912; Nickel, 1977) roscoelite-ankerite-quartz-siderite-hematite-

pyrite-tellurides, containing up to 100,000 g/t Au.

Gauthier et al. (in revision) further differentiated Fimiston lodes into four

paragenetic stages, based on cross-cutting relationships and alteration assemblages.

Stage I predates gold mineralization and comprises cockade and crustiform carbonate-

magnetite±chlorite and hematite veins and breccias. Stages 2 to 4 are the gold bearing

stages and comprise the following: (Stage 2) gold- and telluride-hosting pyrite-

tourmaline-magnetite-chlorite-carbonate replacement veins; (Stage 3) gold- and

telluride-hosting banded quartz-carbonate extension veins with open-space filling

textures, and pervasive quartz replacement; and (Stage 4) thick quartz-carbonate veins

with a gold and telluride-bearing sericite-carbonate-pyrite vein selvedge, although the

gold content of these veins decreases distal to the deposit.

Three distinct alteration types (Mikucki and Heinrich, 1993), which vary with

depth and which crosscut the earlier chlorite carbonate alteration, characterize the Mt


144

Charlotte quartz-carbonate-scheelite vein deposit. At shallow levels, <450m depth

below contemporary ground level, type 1 alteration comprises ankerite-sericite-pyrite-

siderite-rutile in the inner zone, and albite-chlorite-magnetite-pyrite in the outer zone.

Type 2 alteration (600-800m depth) comprises proximal ankerite-sericite-pyrite-

siderite-rutile-(pyrrhotite) and distal albite-chlorite-magnetite-pyrrhotite, and is

transitional to type 3 alteration (>800m depth), which comprises proximal ankerite-

sericite-albite-pyrrhotite-siderite-rutile-(pyrite) and distal albite-chlorite-magnetite-

pyrrhotite. Pyrrhotite increases in abundance at the expense of pyrite with increasing

depth and temperature, and proximity to the ore bodies.

A number of different alteration events at different scales are recognized at St

Ives. The earliest recognized event is syn-volcanic to early deformation-related (De to

D1) seawater spilitization of the greenstone sequence, particularly in the Foster thrust

area (Nguyen, 1997), to the south of Kambalda. Regional carbonate alteration

associated with D2-D3 deformation along the BLFZ is ubiquitous to the region

(Bartram and McCall, 1971; Phillips, 1986; Barley and Groves, 1987). Neumayr et al.

(2008) recognized a pre-gold skarn-type epidote-magnetite-pyrite-chalcopyrite-quartz

assemblage spatially associated with, and forming a contact aureole to, barren porphyry

stocks. At the deposit scale, Neumayr et al. (2008) described three gold-related

alteration assemblages:(1) Stage 2a reduced pyrrhotite-carbonate-amphibole-biotite ±

quartz ± arsenopyrite ± pyrite; (2) Stage 2b oxidized plagioclase-Fe-carbonate-pyrite-

chalcopyrite ± Au ± magnetite ± hematite, and (3) late- to post-main gold quartz (vein)

± pyrite ± chlorite ± Au ± carbonate. Clark et al. (1986) described post-D3 metasomatic

biotite and retrograde carbonate alteration associated with gold mineralization at the

Victory deposit.

Widespread carbonate (dominantly calcite) alteration, unrelated to gold

mineralization, is ubiquitous throughout the New Celebration mine sequence (Norris,

1990) and likely represents regional scale, fault controlled mantle carbonate associated

with D2-D3 deformation on the BLFZ (cf. Bartram and McCall, 1971; Phillips, 1986;

Barley and Groves, 1987). At the deposit scale, early metamorphic magnetite alteration,

hosted within S3NC (NC denotes the regional equivalent at New Celebration) foliation

planes and associated with D3NC deformation, (Nichols, 2003) pre-dates Stage I

mineralization. Nichols (2003) identified two gold-related alteration assemblages: (1)

Stage I gold-related ankerite-biotite-pyrite ± albite alteration; and (2) Stage II Au-

related albite-ankerite-sericite-pyrite ± magnetite ± hematite alteration. Nichols (2003)


145

and Nichols et al. (in revision) recognized a number of post-gold alteration

assemblages: (1) coarse-grained, anhedral, elongate hornblende locally developed in

fractures with M1 porphyry dikes; (2) coarse-grained, euhedral, disseminated actinolite-

tremolite overprinting D3 deformation fabrics and closely associated with the M2

porphyry margins, and (3) coarse-grained, euhedral carbonate, which overprints all

other alteration assemblages.

4.4 Hydrothermal Fluid Chemistry Associated with Gold Mineral Systems in the Kalgoorlie-Kambalda Corridor A number of fluid inclusion studies have been undertaken at the New

Celebration, Kalgoorlie and St Ives deposits. The results of these studies are

summarized in Table 7.3 and Fig. 7.7.

Ho (1987) and Ho et al. (1990) reported mixed (30-50 mole % CO2) low salinity

(<5.5 equiv. wt. % NaCl) fluid inclusions from both Fimiston and Oroya-style

mineralization, and noted that the inclusions associated with the Oroya lodes contained

significant methane. They postulated formation pressures and temperatures between 1.0

to 4.0 kbars and 90 to 230° C for Fimiston-style mineralization and 3.1 to 3.4 kbars and

225-335° C for Oroya-style mineralization. In contrast, Clout (1989) reported much

lower formation pressures, between 0.3 and 0.5 kbars, from concomitant aqueous,

mixed and CO2-rich inclusions, which he interpreted to represent 2 episodes of phase

separation. This formed the basis of his hypothesis that the Fimiston and Oroya lodes

were of epithermal genetic origin. Bateman et al. (2001) and Bateman and Hagemann

(2004) later questioned Clout’s calculations of paleopressures as no L/V ratios were

documented and questionable equations of states for isochore calculations were used.

Fluid inclusion, mineral equilibria, and calcite-dolomite geothermometry

indicate that gold mineralization at the Victory deposit in St Ives occurred at

temperatures and pressures between 340° C and 430° C and 1.7 to 2.0 kbars,

respectively (Clark et al., 1989). K. Petersen (pers. com. 2007) analyzed fluid inclusions

from a number of St Ives deposits and inferred formation conditions of 440-510° C and

1.7-


146

Table 7.3 Summary of the hydrothermal fluid, alteration, P-T-X and stable isotopic characteristics of the Golden Mile, New Celebration and St Ives gold camps Th °C

(FI) T °C (ME)

Pressure MPa (FI)

Pressure MPa (ME) XCO2 XCH4

Salinity (eq. wt% NaCl) pH

log ƒO2 log ƒS2 d13C d18O dD d34S

New

Cel

ebra

tion

Pre-gold 270 to 500

100 to 300

0.16 ± 0.06 0 2.7 ± 1.0

Stage I

300 to 390

320 to 400

0.1 ± 0.01 to

0.33 ± 0.13

0.0 to 0.3

±0.01

1.9 ± 1.2 to

5.9 ± 0.7

-7.6 to +3.8

Stage II

280 to 320

80 to 320

0.16 ± 0.03 to

0.53 ± 0.28

0.0 to

0.06

3.6 ± 0.3 to

5.73 ± 1.0

-10.6 to -3.2

Post-gold (high salinity)

100 to 180 40 to 100

18.4 ± 0.1 to

22.3 ± 0.9

St Iv

es

Stage I 219 to 276 (no PC)

0.8 to 7.3

Stage II RO

0.0 to 0.95

0.05 to 1.0

-2.30 to +1.75 (4.05)

Stage II OR 268 to 277 (no PC)

0.95 to 0.99

0.0 to 15.2

-2.78 to -0.17 (2.61)

Stage III 53 to 337 (no PC)

0.95

0.0 to 37.0

Victory 340 to 400 350 to 430

140 to 200 < 200 0.1 to 0.2 8 to 9

-5 ± 2

+8.9 to + 13.3

-30 ± 12

-6.26 to +5.10 (11.36)


147

Gol

den

Mile

Oro

ya S

tyle

van-mu-tell-qtz-py-mag-hem-cc-(ab-apy) 100,000 g/t Au

225 to 355 305 to 340 (cl)

120 to 280 30 to 220

<5

-3.1 to +5.6 (py)

Cha

rlotte

Sty

le

Type 1 alteration 200 to 320

none <4

Type II alteration 120 to 280

up to 0.5

Type III alteration up to 440

up to 0.5

not differentiated

150 to 230

0.25 to 0.3

2.0 to 5.5

5.8 to 6.1

-28.8 to -33.4

-8.2 to -10.5

-7.9 to -1.6

10.9 to 11.9

-4.2 to +1.0

FI = fluid inclusion; ME=mineral equilibria; PC= pressure correction; ank=ankerite; ser=sericite; py=pyrite, tell=telluride, van-mu=vanadian muscovite, qtz=quartz, mag=magnetite, hem=hematite, cc=calcite, ab=albite, apy = arsenopyrite, cl=chlorite, ahy=anhydrite

Th °C (FI)

T °C (ME)

Pressure MPa (FI)

Pressure MPa (ME) XCO2 XCH4

Salinity (eq. wt% NaCl) pH

log ƒO2 log ƒS2 d13C d18O dD d34S

Gol

den

Mile

Fim

iston

Sty

le

ank-ser-py-tell alteration 1-10,000 g/t Au 190 to 230

(no PC) 340 to 390 (aspy)

360 to 380 (cl)

105 to 400

110 to 290

<4.5

-10.44 to +29.9 (py)

qtz-hem alteration 0.1 - 3 g/t Au

160 to 240

100 to 240

<5.5

not differentiated

0.2

-37 to -27

10-38 to 10-14 (mH2S)

-6.7 to -0.2

8.6 to 15.0

-26 to -44

+12 to +18 (ahy)


148

Figure 7.6 Trapping conditions for ore-stage fluids from the Golden Mile, New Celebration and St Ives

gold camps. All show declining pressure and temperature with time

4.0 kbars for pre-gold Stage 1, 205-310° C and 0.7-2.1 kbars for the gold related Stage

2a and 2b events and 120-300° C and 0.1-1.6 kbars for the post-gold Stage 3 fluids,

based on analyses of low salinity (<7 equiv. wt. % NaCl) aqueous and moderate salinity

(up to 15 wt.% NaCl equiv.) aqueous-carbonic inclusions.

Hodge et al. (in revision) demonstrated a complex and protracted fluid history

for the New Celebration gold deposit (Table 7.3, Fig. 7.7). Pre-gold methane and

aqueous-carbonic inclusions indicate formation temperatures and pressures between 270

to 500° C and 1 to 3 kbars. Stage I gold mineralization formed from a mixed H2O-CO2-

NaCl fluid at temperatures and pressures between 330 °C and 390 ° C and 3.2 to 4.0

kbars, respectively. Stage II gold mineralization formed from mixed aqueous-carbonic

fluids at temperatures and pressures between 280 to 320° C and 0.8 to 3.2 kbars,

respectively. Coeval vapor- and liquid-rich fluid inclusions with similar homogenization

temperatures and variable bulk compositions and molar volumes indicated that Stage II

fluids underwent at least some phase separation. Aqueous and methane-dominated

fluids that post-date gold mineralization formed at temperatures and pressures between

100 to 180° C and 0.4 to 1.0 kbar, indicating that they formed in a different P-T

environment to the gold-related inclusions, likely after a period of uplift and erosion,

and significantly after gold mineralization ceased.


149

All three deposits show declining temperatures and pressures with time (Fig.

7.7), presumably reflecting the changing P-T conditions of the terrane as it evolved.

Hodge et al. (submitted) and Clark et al. (1989) concluded that the later stages of gold

mineralization at the New Celebration and St Ives deposits, respectively, took places

significantly later than the earlier stages, after a period of uplift and erosion, indicating

protracted gold mineralization during the evolution of the orogen.

4.5 Carbon, Oxygen and Hydrogen Stable Isotopes The following section summarizes the stable isotopic data of Golding (1982,

1984), Clout (1989) and Golding et al. (1990a; 1990b) from the Golden Mile and Mt

Charlotte deposits in Kalgoorlie and the Victory deposit in Kambalda (Table 7.3). There

are no available data on the C, O or H isotopic compositions from New Celebration.

Golding (1982, 1984) analyzed the carbon isotopic composition of gold-related

carbonates from the Golden Mile and Mt Charlotte deposits in Kalgoorlie and the

Victory deposit in Kambalda. She concluded that the recalculated ore-fluid values fell

within the range of magmatic carbon and that the likely fluid source for both the

Kalgoorlie and Kambalda deposits was most consistent with a magmatic CO2 reservoir.

Oxygen and hydrogen stable isotope data from the Golden Mile are sparse,

contradictory and poorly constrained. Golding et al. (1990a; 1990b), calculated the

18Ofluid composition from quartz vein, vein carbonate and wall rock quartz and

carbonate alteration from the Golden Mile No. 4 Lode, and from the Mt Charlotte

deposit. Using a model formation temperature of 350±50° C, they postulated either a

metamorphic or a magmatic origin for the ore fluids at both the Golden Mile and Mt

Charlotte, but could not differentiate further. Clout (1989) calculated the 18Ofluid and

Dfluid of ore-related quartz veins and muscovite for Fimiston style mineralization at

180° C. In combination with his fluid inclusion data, he used these data to infer that the

Fimiston ore fluids were of seawater or low-latitude meteoric water origin, which

underwent isotopic exchange with wall rocks or a magmatic fluid, and proposed a near-

surface epithermal origin for the Fimiston and Oroya deposits.

At Victory, Golding et al. (1990b) calculated the 18Ofluid for gold-bearing veins

and gold-bearing wall rocks, and Golding and Wilson (1987) analyzed chlorite in

mineralized Defiance Dolerite from the Victory deposit. They both noted that the

calculated oxygen and hydrogen isotopic compositions of the ore fluids at Kalgoorlie

and Kambalda were within the field of overlap between magmatic and metamorphic


150

waters. Importantly, however, Golding et al. (1990a) noted that the calculated isotopic

composition of ore fluids at Victory was significantly enriched in D relative to the D

of hornblende and phlogopite in Kambalda lamprophyres (Rock et al., 1989). For this

reason, Golding et al. (1990a) rejected magmatic fluids derived from these

lamprophyres as a potential mineralizing fluid source, but did not discount a distal

magmatic source. The stable isotopic evidence presented above suggests a magmatic

contribution to the hydrothermal system at both deposits.

4.6 Sulfur Isotopic Composition and Comparison with Previous Studies The sulfur isotopic composition of syn-sedimentary and ore-stage sulfides from

the Golden Mile and New Celebration was determined to complement existing isotopic

data sets and to further constrain compositions based on newly developed paragenetic

sequences. Thirty-one in situ pyrite and pyrrhotite analyses from nine Golden Mile and

three St Ives samples were analyzed by Nd-YAG laser ablation, following the procedure

of Huston et al. (1995a) at the Central Science Laboratory (CSL), University of

Tasmania. These samples represent synvolcanic sulfide from Kalgoorlie, four

paragenetic stages of Fimiston type gold mineralization (Golden Mile), and different

hydrothermal alteration assemblages from the Conqueror and Revenge deposits (St

Ives). All results are reported in parts per thousand (per mil, ‰) relative to the Canyon

Diablo Troilite (CDT). The results of this study are compared with previous studies on

sulfides from the Golden Mile (Lambert et al., 1984; Clout, 1989; Hagemann et al.,

1999; Bateman et al., 2001; Bateman and Hagemann, 2004), New Celebration (Hodge

et al., in revision) and St Ives (Palin and Xu, 2000; Hodkiewicz, 2003; Walshe et al.,

2006; Neumayr et al., 2008) (Table 4).

4.6.1 Golden Mile

The results of this study on pre-gold and four paragenetic stages of Fimiston-

style gold mineralization showed a broad range of δ34S values (Table 7.4, Fig. 7.8), both

within and between samples, and displayed significant variability according to host

rock, alteration assemblage and paragenetic relationship. Synvolcanic pyrite had sulfur

isotopic ratios from +3.2 to +4.2 per mil (n=2). Fimiston sulfides showed the broadest

range in values, -10.4 to


151

Table 7.4 Summary of the sulfur isotopic compositions of sulfides from Golden Mile (GM), New

Celebration (NC) and St Ives (SI)

Deposit Style Mean/Std Dev Min/Max/Spread

Method Source

NC Mylonite +1.83 ± 1.22 +0.57 to +3.77 (3.2) LA Hodge et al. (in revision)

Porphyry -5.89 ± 1.54 -7.49 to -3.15 (4.3) LA Hodge et al. (in revision)

Contact -5.90 ± 1.98 -8.34 to -3.22 (5.12) LA Hodge et al. (in revision)

Fracture -8.97 ± -1.34 -10.61 to -7.40 (3.21) LA

Hodge et al. (in revision)

-3.0 ± 5.2 -8.64 to +5.54 (14.8) LA Hodkiewicz (2009)

GM Synvolcanic sulfide +4.10 ± 0.72

+3.59 to +4.61 (1.02) LA This study

Fimiston Stage I +2.40 ± 0.81 +1.82 to +2.97 (1.15) LA This study

Fimiston Stage II +5.33 ± 8.95 -7.21 to +15.68 (22.89) LA This study

Fimiston Stage III -7.63 ± 1.89

-10.44 to -4.65 (5.79) LA This study

Fimiston Stage IV -0.92 ± 2.74

-2.87 to +2.21 (5.08) LA This study

Depth-HG +1.3 ± 4.8 -4.7 to +10.3 (15.0) LA Bateman et al. (2000) GBM - HG +4.0 ± 5.5 -3.8 to + 9.2 13.0) LA Bateman et al. (2000) GBM - Prox +2.7 ± 3.4 -3.5 to + 8.2 (11.7) LA Bateman et al. (2000) GBM - Dist +2.9 ± 1.9 -1.6 to +4.2 (5.8) LA Bateman et al. (2000) LV - HG -3.3 ± 2.3 -8.8 to + 1.0 (9.8) LA Bateman et al. (2000) LV - Prox -4.2 ± 2.5 -7.9 to -2.1 (5.8) LA Bateman et al. (2000) LV - DP -4.2 ± 1.6 -6.0 to -3.2 (2.8) LA Bateman et al. (2000) LV - Dist +1.8 ± 2.1 0.0 to +4.9 (4.9) LA Bateman et al. (2000) Oroya - HG +3.6 ± 1.4 +2.3 to +5.1 (2.8) LA Bateman et al. (2000) Oroya - Prox +2.2 ± 2.7 -3.1 to- +4.9 (8.0) LA Bateman et al. (2000) Oroya - Dist +3.3 ± 2.5 -0.9 to +5.6 (6.5) LA Bateman et al. (2000) Mt Charlotte +3.0 ± 0.9 +2.2 to +4.3 (2.3) Golding et al. (1990)

SI Revenge Reduced +0.2 ± 1.8

-2.30 to +1.75 (4.05) LA This study

Revenge Oxidized -1.6 ± 1.0 -2.78 to -0.17 (2.61) LA This study

Victory -0.3 ±2.6 -4.4 to +5.1 (9.5) LA Palin and Xu (2001)

Victory-Defiance -3.8 ± 1.5 -6.26 to -1.16 (5.1) LA Hodkiewicz et al. (2009)

Victory-Defiance 3.1 ± 1.4 -5.5 to -1.5 (4.0) LA Ho et al. (1994) Victory-Defiance -4.1 ± 1.4 -6.3 to -1.2 (5.1) CONV Ho et al. (1994)


152

Figure 7.7 Composition of sulfides from different lodes and different paragenetic events at Golden Mile,

different alteration assemblages at St Ives and different mineralization stages at New Celebration


153

+15.7 ‰ (n=19) with the most depleted values coming from a gold-telluride quartz-

carbonate vein (Stage III of Gauthier et al. (in revision)) and the most enriched from a

pyrite-tourmaline vein fragment within a mafic dike (Stage II of Gauthier et al. (in

revision). Lambert et al. (1984), Phillips et al. (1986) and Clout (1989) also established

significantly depleted sulfur isotopic compositions (< -10 ‰) of pyrite, using

conventional bulk sulfur isotopic analytical methods, for Fimiston-style gold

mineralization at the Golden Mile.

The results of this study indicate that sulfide formation and gold precipitation at

Fimiston took place during fluctuating and highly variable ƒO2 conditions, likely either

as a combination of ore-forming processes and/or involving a number of different sulfur

sources (Bateman et al., 2001; Bateman and Hagemann, 2004). The significantly

depleted isotopic compositions reported from the Fimiston lodes suggest an oxidized

magmatic fluid source, (cf. Cameron and Hattori (1987) and Clout (1989), who

proposed an intrinsically oxidized, magmatic ore fluid to account for the isotopic

variation reported from the Fimiston lodes, and are consistent with those of Hagemann

and Bateman (2001), who concluded that gold precipitation at the Golden Mile occurred

as the consequence of wall rock sulfidation and phase immiscibility and that sulfur

likely was derived from several sources. They concluded that the pyrite isotopic

composition of the Oroya lodes, in particular, was consistent with formation by mixing

an oxidized magmatic fluid with heavy sulfur derived from the metasedimentary units

within the Paringa Basalt.


Hodkiewicz (2003), Hodkiewicz et al. (2009) and Hodge et al. (in revision),

reported predominantly depleted sulfur isotopic values from ore-stage pyrites at New

Celebration. Sulfur isotope values from Stage I-related pyrites ranged between -7.6 per

mil and +3.8 per mil (n=14) and Stage II pyrites ranged between -10.6 per mil and -3.2

per mil (n=16). Hodkiewicz (2003) and Hodkiewicz et al. (2009) documented a broad

negative correlation between 34S and gold grade (r2=0.73, n=5) at New Celebration and

concluded that carbonation reactions between the ore-fluid and wall rock magnetite and

hematite initiated fluid oxidation, however Hodge et al. (in revision) using a much

larger database demonstrated no such correlation (r2=0.10, n=30). Further, Mikucki

(E.J. Mikucki unpub. report, 2001) has shown that magnetite carbonation would only

lead to ore fluid oxidation at very low fluid/rock ratios, which is incompatible with the

significant hydrothermal fluid flow and high fluid/rock ratios expected within a crustal


154

scale fault system such as the BLFZ. Hodge et al. (in revision) confirmed that the

sulfidation of iron-rich wall rocks was the mechanism by which all of Stage I, and at

least part of Stage II gold, precipitated at New Celebration. As this mechanism would

not effect a change to the oxidation state of the dissolved sulfur species (Palin and Xu,

2000), Hodge et al. (in revision) concluded that the sulfur isotopic composition of the

majority of ore-stage pyrite at New Celebration reflected the ore fluid composition, and

that the negative isotopic composition suggested possible magmatic contributions to the

ore fluid, at least during Stage II. Hodge et al. (in revision) documented intermittent

phase immiscibility during Stage II gold mineralization and concluded that fluid

oxidation during phase separation accounted for both the negative sulfur isotopic

composition and the spread in δ34S ratios observed in Stage II ore-related pyrites.

4.6.3 St Ives

The results of this study did not differentiate the pre-gold and syn-gold samples

based on their isotopic composition (Fig. 7.8, Table 7.4). Pyrite from both the pre-gold

amphibole-pyrrhotite veins and the Stage 2b ore zone related alteration assemblages

showed significant overlap, with δ34S values ranging from -2.3 to +1.8 per mil and -2.8

to -0.8 per mil respectively. These values are, however, within the range of reported

average means of sulfides from Yilgarn Craton deposits (Hodkiewicz, 2003;

Hodkiewicz et al., 2009) and well within the ranges reported by other researchers (Ho et

al., 1994; Palin and Xu, 2000; Hodkiewicz, 2003; Hodkiewicz et al., 2009) in the St

Ives gold field.

Palin and Xu (2000) ,Hodkiewicz (2003) and Hodkiewicz et al. (2009)

documented a negative correlation between total gold concentration and 34S in pyrite.

Palin and Xu (2000) concluded that fluid oxidation occurred in situ during gold

mineralization by carbonation reactions between wall rock magnetite and the ore fluid.

Hodkiewicz (2003) documented different isotopic compositions in differently oriented

structures – isotopically depleted pyrites were observed in gently dipping structures,

whereas enriched pyrites were observed in the steep structures. He invoked large-scale

pressure fluctuations in the more dilatant shallow dipping structures to account partially

for the depleted isotopic compositions. Neumayr et al. (2008) reported 34S ranges in

pyrite, chalcopyrite and pyrrhotite (in situ LA-ICP-MS analyses) from -8.4 to +5.1 per

mil at the St Ives gold camp. The most negative 34S values were associated with an

oxidized magnetite domain (determined by a geographical information systems (GIS)

interpretation of the drill core database) and the most positive values with a reduced


155

pyrrhotite domain. They postulated that gold mineralization was consistent with mixing

between an oxidized, magmatic-derived fluid and a reduced hydrothermal fluid and

concomitant sulfate reduction and methane oxidation. Results of these studies indicate

that a significant magmatic fluid component was a factor in gold mineralization at all

three deposits.

4.7 Mineral Chemistry of Sulfides, Oxides and Gold Associated with Gold Mineral Systems in the Kalgoorlie-Kambalda Corridor Thirty-seven samples from the Golden Mile, representing syn-volcanic sulfides,

different mineralization styles (Fimiston and Oroya), different lode systems (East, West

and Aberdare), different chronological events within a single lode system (Fimiston

Stages I-IV), and shallow vs. deep > (600m below current surface) samples, 11 samples

from New Celebration representing Stage I and Stage II ore-related sulfides, gold and

Fe-oxides, and 11 samples from St Ives, representing different hydrothermal alteration

fluid systems, were analyzed at the ARC Centre for Excellence in Ore Deposits at the

University of Tasmania, using the method described in Appendix 8. The samples were

analyzed for 26 major and trace elements to identify similarities and differences of gold

mineralization at the Golden Mile, New Celebration and Kambalda deposits and within

different paragenetic and/or mineralization stages within individual deposits.

4.7.1 Golden Mile

Pyrites from all lodes in the Golden Mile are high in As relative to Ni and Co

(Fig. 7.9). Fimiston Stage II pyrites contain the lowest average As concentrations, and

pyrites from the deepest lodes (>600 m below the current surface) contain the highest

average As concentrations. Broad peaks for Au, Ag and Te in pyrites from the Lake

View and Aberdare lodes, and the deep lodes indicate that these elements are contained

primarily within the pyrite lattice, either as stoichiometric or non-stoichiometric

substitutions for Fe (Au, Ag) or S (Te). Pyrites from these lodes also had the lowest

average Ag and Te concentrations of all the Golden Mile pyrites, and contained only

rare poly-metallic sulfide inclusions. Pyrite from other lodes contained Au, Ag and Te

as mineral inclusions, as evidenced by narrow spiky peaks, and had higher average Ag

and Te concentrations than those in which gold was contained within the pyrite crystal

lattice. Fimiston Stages II and IV pyrites showed strong positive correlations between

Au and As, which were not evident in pyrites from any other lode.


156

Gold grain analyses from Fimiston and Oroya style mineralization revealed that

Au commonly contains Cu and also showed that Te is not part of the Au crystal

structure, but instead occurs as inclusions within the grains, commonly with Pb and Sb

Iron oxides from the Fimiston, Lake View, Aberdare and deep lodes had

complex chemical compositions, and were commonly zoned with respect to Ti, W, Sb

and Co. They also contained Zr inclusions. Magnetites from the Great Boulder Main

lode had very simple chemical composition, with no trace element enrichment evident

in the analyses either as inclusions or as substitution. Pyrites in the Fimiston, Lake

View, Aberdare and the deep lodes showed corresponding enrichments in the same

elements evident in the oxides, suggesting that dissolution of magnetite during wall rock

sulfidation reactions contributed significantly to the chemical signature of the ore-stage

pyrite. Pyrites from the Great Boulder Main lode were also geochemically very simple,

reflecting the lack of trace elements in magnetite, however, the pyrite had elevated As

concentrations not evident in the magnetite, suggesting that As was contributed to the

pyrite by the ore forming fluid.


New Celebration ore-stage pyrites from both Stage I and Stage II contain Ni and

Co, but trace to no As (Fig. 7.9). Stage I ore-stage pyrites also contained lattice bound

Ti, W, Pb, Zn, Cr, and minor As. Titanium, Mn, Cr, Zn, Cu, W, Mo, Au, Ag, As Te, Sb,

Bi, U, Th, La and Zr commonly occurred as inclusions in both Stage I and Stage II

pyrites, which also contained Au, Ag, Te and Pb associated together, reflecting the

presence of Au-Ag-Pb tellurides. This is consistent with petrographic and SEM

observations of Nichols (2003) who reported hessite (AgTe2), altaite (PbTe), melonite

(Ni2Te) and tetradymite (Bi2Te2) from Stage I ore-stage pyrites.

Gold analyses revealed minor chemical differences between Stage I and Stage II.

Stage I gold contained only silver within the lattice, whereas Stage II gold contained Pb

and Cu, in addition to Ag, within the crystal lattice. Gold and Ag showed a strong

positive correlation with each other in all mineralization styles except Stage I Mylonite-

style. Stage II Contact-style pyrite showed a strong positive correlation between Au and

Te, which was not observed in any other mineralization style. Stage II gold grains


157

Figure 7.8 Ternary Ni-Co-As plot for pyrites from the Golden Mile (left), New Celebration (center) and

St Ives (right). Golden Mile pyrites contain relatively more arsenic than those from New Celebration or St

Ives.

also hosted rare Pb-Bi and Ba-bearing inclusions, which likely represent sulfide (galena)

and sulfate (barite) inclusions within the gold grains, consistent with petrographic

observations made in this study and (Nichols, 2003).

Metamorphic magnetite from Stage I mineralization-hosting sheared

intermediate porphyries comprised ubiquitous Ni and Co, in addition to Ti, Cr, Zn, As,

Bi and W in variable proportions within the magnetite crystal lattice. They also

contained abundant poly-metallic (Pb, Ti, Cr, Bi, Ba, Sb, W, Mn, Zn-bearing) and

zircon inclusions. In contrast, hydrothermal magnetites and ilmenites in mafic volcanic

rocks were compositionally simple and typically contained only zircon inclusions.

A spider diagram (Fig. 7.10) of elemental abundances relative to average crustal

abundances in pyrites from all mineralization styles, metamorphic magnetite and

hydrothermal Fe oxides from high Mg basalt and dolerite, clearly illustrates that the

trace element composition of pyrites from Stage II Fracture-style mineralization are

markedly different from Stage I or Stage II Contact-style pyrites. Petrographic and fluid

inclusion evidence (Hodge et al., in revision) indicate that all of Stage I, and Stage II

Contact-style mineralization formed by reaction of gold- and sulfur-bearing ore fluids

with iron-rich wall rocks whereas Stage II Fracture-style gold precipitated via phase

immiscibility. The variability observed in the different ore stage pyrites therefore likely

reflects different degrees of influence from wall rock oxides and ore fluids. The

composition of those pyrites that formed by reactions with magnetite and ilmenite (i.e.

Stage I and Stage II Contact-style) reflects the composition of the oxides, whereas the

composition of Stage II Fracture-style pyrites more closely reflects the composition of

the ore fluid. This is consistent with the observations of Phillips et al. (1986; 1988) from

the Golden Mile, who


158

Figure 7.9 Spider diagram illustrating the abundances of all the elements analyzed, except Fe, relative to

average crustal abundances (data from Rosler and Lange, 1972) in pyrites from Stage I (Mylonite- and

Porphyry-style) and Stage II (Contact- and Fracture-style) mineralization, in addition to metamorphic

magnetite from mylonitized monzonite and hydrothermal Fe-oxides from high-Mg basalt and dolerite,

illustrating that pyrites from Stage II Fracture-style mineralization show markedly different trace element

patterns than those pyrites related to both Stage I mineralization styles and Stage II Contact-style

mineralization. This likely reflects differing contributions from wall rocks and ore fluids for the different

mineralization styles and events.

concluded that the composition of pyrite that precipitated from fluids that had dissolved

oxides or carbonates would reflect the composition of those oxides or carbonates.

4.7.3 St Ives

St Ives pyrites contain ubiquitous Ni and Co, however, in contrast to the Golden

Mile samples, St Ives pyrites contain less As relative to Ni and Co (Fig.7.9). Post-gold

Stage 3 pyrites contain only Fe and Co, whereas porphyry-related Stage 1 pyrites, and

gold-related Stage 2B pyrites also contain Ni and As in varying proportions. Gold, Ag,

Te and other elements are present only in low concentrations, and Au does not correlate

with either Ag or Te. Zonation of inclusions is evident in some ore-stage sulfides;

inclusion rich cores contain Au, Ag, Te and other poly-metallic sulfides, whereas

inclusion-free rims contain only Fe, Ni and Co.


159

4.7.4 Discussion

Nickel and cobalt are ubiquitous in all pyrites analyzed, however, pyrites from

the Fimiston and Oroya lodes show a number of contrasts in other trace element

abundances to those analyzed at New Celebration and St Ives. Fimiston and Oroya lode

pyrites contain abundant As relative to Ni and Co, which is not observed in New

Celebration or St Ives pyrites. Fimiston and Oroya pyrites are high in Sb, but contain

little or no Bi, and Te occurs in Fimiston and Oroya pyrites at concentrations several

orders of magnitude higher than in pyrites from either New Celebration or St Ives.

Nickel and cobalt are contributed by the wall rock, and concentrations correspond

directly to the host rock, for example, at New Celebration, pyrites from Contact-style

mineralization, which formed by wall-rock reaction with oxides in high-Mg basalt, have

higher Ni and Co concentrations than pyrites from Fracture-style mineralization, which

formed by phase separation. Evidence from New Celebration also indicates that the

composition of ore forming pyrites is in part controlled by the composition of wall rock

iron oxides, at least where wall rock reaction is the dominant ore forming process. Other

elements, such as Au, Ag, Bi, Pb, As and Te are contributed by the ore fluid (Ho et al.,

1995).

Thermodynamic modeling by Cooke and McPhail (2001) predicted that Te is

most readily transported in magmatic hydrothermal vapors, therefore, the high Te

concentrations reported at the Golden Mile suggest a magmatic fluid source. Cooke and

McPhail (2001) determined that the solubility of aqueous Te species (H2Te(aq), HTe-

and H2TeO3 (aq)) is low in aqueous fluids and maintain that the only viable mechanism

for depositing Te-rich ores is via the condensation of Te2(g) and H2Te(g) from

magmatic vapors into precious metal brines where they react with aqueous gold-bearing

complexes (Au(HS)–2 or Au(HS)) to form gold-telluride deposits.

Fimiston and Oroya ore-related pyrites at the Golden Mile contain

characteristically high concentrations of As and Sb. Antimony enrichment is common in

terranes dominated by metasedimentary sequences and has been recognized in the

Phanerozoic orogenic lode gold deposits in the South Island of New Zealand (Pitcairn et

al., 2006) and the North American Cordillera (Goldfarb et al., 1993), in Archean

mesothermal gold deposits of the Superior Province in Canada (Colvine, 1989), the

Kwetke region of Zimbabwe (Buchholz et al., 2007) and in the epizonal Wiluna deposit

in the Yilgarn Craton (Hagemann et al., 1993; Hagemann and Lüders, 2003). Both As

and Sb are highly soluble in hydrothermal solutions as hydroxoantimonite or oxyanions


160

over a broad range of temperature, pH and ƒO2 conditions. Generally, antimony

precipitates at shallow crustal levels (Nesbitt et al., 1986; Nesbitt and Muehlenbachs,

1989; McCuaig and Kerrich, 1998) and enrichment of pyrite in Sb takes place at

temperatures between 200 and 300° C (Pitcairn et al., 2006). The source of Sb in

deposits around the world remain equivocal; Buchholz et al. (2007) considered that

local metabasalts and metasedimentary rocks provided the As and Sb at Kwetke,

whereas Pitcairn et al.(2006) determined that As and Sb in the Otago schist-hosted

deposits of New Zealand was derived from the surrounding country rock during

prograde metamorphism. Regardless of the source, the presence of Sb in Fimiston and

Oroya pyrites suggests emplacement at epizonal crustal levels and at temperatures

<300° C.

5. EVOLUTION OF THE BOULDER-LEFROY FAULT ZONE AND ITS

POTENTIAL ROLE IN THE LOCATION OF GOLD

MINERALIZATION IN THE KALGOORLIE-KAMBALDA CORRIDOR

Despite over 100 years of gold exploration in the Kalgoorlie-Kambalda corridor,

and almost as many years of study into the geology of the deposits comprising one of

the richest gold endowed areas of the world, no research projects have drawn together

the abundant available structural, mineralogical and geochemical data to evaluate the

exact role of the BLFZ with respect to the location of gold mineralization within the

Kalgoorlie-Kambalda corridor. This section presents a synthesis of the existing data

(Figs. 7.10-7.16), and new data presented in section 4, to evaluate the potential role of

the BLFZ in forming the giant and world-class deposits that make the Kalgoorlie-

Kambalda corridor so unique.

5.1 D1- early D2 (>2675 – 2670) The early history of the BLFZ is contentious. Gee et al.(1981) considered that

the BLFZ originated during early, E-W extension (De), as a feeder fault for greenstone

belt volcanism. Other authors, for example Swager (1989) and Weinberg et al. (2005)

did not consider that the BLFZ was active as a regional scale crustal structure prior to

regional D2. Swager (1989) argued that: (1) the fault occupies the axial plane of the

regional D2 Celebration anticline, therefore faulting alone cannot account for the

change in younging direction across the fault; (2) at Kambalda the BLFZ crosscuts the

eastern limb of the Kambalda anticline; and (3) the BLFZ offsets the D1 Feysville and

Mt Hunt faults south of Kalgoorlie. Weinberg et al. (2005) observed that: (4) the earliest


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recognized deformation phase of the BLFZ at New Celebration was steeply dipping

north-south oriented thrust faulting; and (5) that the interpretation of seismic images in

the Kalgoorlie area indicated that the BLFZ formed as a series of unconnected north-

south oriented thrust ramps arranged roughly along the strike of the present BLFZ.

Recent work by the Predictive Mineral Discovery Cooperative Research Centre

(pmd*CRC) in Australia (Miller et al., 2009) indicates that the Lefroy segment of the

fault at Kambalda originated as an east-dipping extensional fault, that formed at least

during the formation of the Black Flag Group rocks, and possibly as early as syn-mafic-

ultramafic volcanism during pre-D1 extension. This interpretation raises a discrepancy

in orientation on the fault system, i.e. the BLFZ dips to the east at St Ives, but changes

orientation to become west dipping at New Celebration and Kalgoorlie (Goleby et al.

2000). This raises the question as to whether the Boulder fault west of the Golden Mile

and the Lefroy Fault east of St. Ives have been correctly linked.

Bateman et al. (2001) and Bateman and Hagemann (2004) proposed a late D1

timing for the Fimiston lodes at Kalgoorlie based on the following: (1) Fimiston lodes

are crosscut by all structures except for the felsic dikes, which are themselves

mineralized; (2) D2 faults clearly cut Fimiston lodes; (3) the regional D3 Adelaide fault

cuts the Fimiston Lake View lode. The findings of Gauthier et al. (2004; in revision),

based on a detailed structural analysis of several underground levels at the Golden Mile

and geochronology of intermineral dike suites supported the early timing of Golden

Mile mineralization. They based their conclusions on the following: (1) the Adelaide

fault cross cuts the pre-D3 Australia East fault, which itself offsets the Fimiston lodes;

and (2) pre-ore feldspar porphyry dikes are dated at 2676±3 Ma (U-Pb TIMS on

zircons) and hornblende-phyric andesite dikes, which crosscut Fimiston ore dated at

2663±11 Ma (U-Pb TIMS on zircons), constraining Fimiston-style gold mineralization

to between 2674 and 2652 Ma. Based on this evidence Fimiston gold lodes formed

much earlier than previously postulated, during D1-D2 compression and potentially

prior to the establishment of the BLFZ as a singular, regionally extensive, crustal-scale

shear zone.

Lungan (1986), Bateman et al. (2001) and Bateman and Hagemann (2004)

proposed an early D2 origin for the Oroya shoot based on the following evidence: (1)

Oroya lode-related faults crosscut and deform the Fimiston-style lodes; and (2) the Main

Lode, Kalgurli and North Kalgurli regional D3 faults offset the Oroya shear zone and

deformed the lodes. In contrast, McNaughton et al. (2005) interpreted a late D3 origin


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for Oroya-style mineralization based on a Pb-Pb zircon age of 2642±6 Ma of a

lamprophyre dike that was interpreted to be emplaced synchronous with the mineralized

tension veins and associated Oroya hanging wall shear zone. However, critical

examination of these data indicate that the dike crosscut Oroya-style mineralization and

was itself cut by Charlotte-style mineralization, therefore, constraining it to be an

intermineral dike (i.e. between two discrete mineralization events), not an

intramineralization dike as McNaughton et al. (2005) had interpreted it.

Fimiston-style gold mineralization (Fig. 7.11) was accompanied by widespread

outer chlorite-carbonate alteration that formed a 1-3km radius halo around the lodes

(Phillips, 1986; Clout, 1989). Clout (1989) constrained this alteration event at 290 to

350° C from a variable salinity (0-23 wt.% NaCl equiv.), low XCO2 (0.02 to 0.06)

mixed aqueous-carbonic fluid, which was likely trapped at the solvus. The broad, low-

grade (<2 g/t Au) haloes in wall rocks adjacent to the Fimiston lodes formed by the

reaction between sulfur-rich ore fluids and wall rock magnetite and iron silicates

(Groves and Phillips, 1987). Pressure-T-X conditions of this alteration event are at

present not constrained. Ho (1987), Clout (1989) and Ho et al. (1990) reported low to

moderate salinity (0-13 wt.% NaCl equiv.) mixed aqueous-carbonic fluid with variable

CO2 contents (XCO2=<0.05 to 1.0), with formation temperatures and pressures between

160 to 250° C and 1 and 3 kbars. These data reflect the formation conditions of the

sericite-ankerite-siderite-quartz-hematite-telluride alteration (type 2 of Clout, 1989) and

roscoelite-ankerite-quartz-siderite-hematite-pyrite-tellurides alteration (type 3 of Clout,

1989). According to Clout (1990) these alteration types are correlated to the narrow

(<1m wide), very high grade (50 to 10,000 g/t Au and locally up to 100,000 g/t Au)

Fimiston lodes.

The Oroya lode and associated Oroya-style mineralization (Fig. 7.12) (Lungan,

1986; Bateman and Hagemann, 2004) formed at temperatures and pressures between

225 and 355° C (Ho, 1987; Ho et al., 1990) and 0.3 to 2.8 kbars (Ho, 1987; Clout, 1989;

Ho et al., 1990), respectively, from a low salinity (< 5.0 equiv. wt. % NaCl) mixed

aqueous-carbonic fluid, which, in contrast to Fimiston-style fluids, contained significant

methane. The origin of methane associated with Oroya style mineralization is at present

equivocal. The methane may be of deep crustal or mantle origin (cf. Duan, 1992) or

may be related to black shale interflow sedimentary rocks, commonly observed

associated with Oroya style mineralization (Scantlebury, 1983; Lungan, 1986; Clout et

al., 1990). If the methane is mantle or deep crustal related, its influx into the Oroya


163

hydrothermal fluid system may reflect the establishment of a mantle connection with the

Golden Mile, either with the formation of the BLFZ in the Kalgoorlie area, or via

another deep crustal structure that has not yet been located or mapped. This deep mantle

connection (cf. Rock and Groves, 1988a, b; Rock, 1990) is supported by the

emplacement of lamprophyre dikes in the Oroya shoot (Mueller et al., 1988;

McNaughton et al., 2005). This interpretation is compatible with the occurrence of

early, pre-gold methane fluid inclusions, observed within the BLFZ at the New

Celebration gold deposit (Hodge et al., in revision)

Brecciation and open-space textures within the lodes, low-temperature silver-

rich tellurides (petzite and hessite, Shackleton et al., 2003)), anhydrite, and the

contemporaneity of high-level andesite dikes with Fimiston-style mineralization

(Gauthier et al., in revision) and depths constrained by the fluid inclusion data of Ho et

al. (1990) indicate that the Fimiston and Oroya lodes formed at paleo-crustal depths of

about 4 to 6 km (cf. Brown and Hagemann, 1995; Gauthier et al., in revision)

The source of the mineralizing fluids at the Golden Mile is poorly constrained at

present, as for orogenic gold deposits in general (cf. Ridley and Diamond, 2000),

however in the absence of a coherent deep-crustal structure, the fluid may have been

derived locally, within, or directly beneath, the Kalgoorlie greenstone terrane. A local

derivation is consistent with the findings of McNaughton et al. (1993) who interpreted

that the Pb isotopic signatures of gold deposits between Menzies and Kambalda, which

were unrelated to major shear zones, reflected derivation from discrete crustal segments

within the greenstone belt sequence. Kent et al. (1995) used Sm-Nd isotopes to invoke a

komatiitic gold source for the Mt Charlotte deposit, again calling upon a locally derived

gold source. Phillips and Groves (1983), Phillips et al. (1987) and Stuwe et al. (1993)

proposed that gold bearing ore fluids in orogenic gold deposits of the Yilgarn craton

resulted from the devolatilization of Archean greenstone belts (i.e. the metamorphic

replacement model). For the Golden Mile, these authors proposed that the greenschist

facies metamorphism in the Kalgoorlie terrane was broadly synchronous with gold

mineralization and provided the hydrothermal fluids and the metals. However, results of

mineral chemistry presented in this paper suggest a magmatic fluid source.

Results of laser ablation ICP-MS analyses on the ore-hosting sulfides in the

Fimiston and Oroya lodes demonstrate a Au-Cu-Te-Sb association, which suggests a

possible felsic magmatic origin (cf. Callaghan, 2001) for the hydrothermal fluids and/or

the metals. The connection to felsic magmatic fluid is consistent with abundant high-Ca


164

and mafic granitoid magmatism in the Kalgoorlie area (Champion and Sheraton, 1997),

which is associated with terrane accretion (cf.Guillemette and Williams-Jones, 1993),

postulated during the time of Fimiston-style gold mineralization. Further evidence for a

link between felsic magmatism and gold mineralization in Kalgoorlie is provided by

Gauthier et al. (in revision) who established that subduction-related calc-alkaline

intermineralization andesite dikes are synchronous with Fimiston-style gold

mineralization.

At Kambalda, D1 deformation involved north-south compression and resulted in

the formation of westerly trending thrust faults and recumbent folds (Archibald et al.,

1978; Swager, 1997). There was no gold mineralization associated with this event at

Kambalda. At the New Celebration gold camp, Nichols (2003), Weinberg et al. (2005)

and Nichols et al. (in revision) did not recognize an event correlating to regional D1.

Based on the current evidence, late D1 and early D2 was the most significant

period for gold mineralization in the evolution of the orogen, with the giant Fimiston

and Oroya lodes formed at the Golden Mile, potentially prior to the establishment of the

BLFZ at Kalgoorlie.

5.2 Late D2 (2670 – 2660) Approximately east-west oriented compression during regional D2 and D3 led to

the upright tilting of conformable stratigraphic units at New Celebration (Nichols, 2003)

and Kambalda (Nguyen et al., 1998), and initiated the formation of the BLFZ at

Kalgoorlie and New Celebration in two stages: firstly, by the development of discrete

approximately north-south trending, east and west dipping thrusts during D2, and

secondly, the reactivation of those thrusts into a single, cohesive, NNW trending,

sinistral oblique-slip shear zone (Weinberg et al., 2005). At Kambalda, D2 deformation

involved the inversion of east-dipping structures formed during rifting and extension

(Miller et al., 2009). Lamprophyres immediately adjacent to, and deformed by, the

BLFZ at New Celebration (Williams, 1994) suggest that the fault was a deep-crustal or

mantle-tapping structure (cf. Rock and Groves, 1988a, b; Rock, 1990). The

development of a regionally extensive deep crustal structure may have been the time

when deep mantle-derived methane was introduced into the hydrothermal system.

Evidence for this includes: (1) primary early, pre-gold methane inclusions in quartz

veins at New Celebration; (2) the appearance of methane in the Oroya ore fluids

(Scantlebury, 1983; Ho, 1986) and; (3) early, pre-gold methane-dominated inclusions at

Kambalda (K. Petersen, personal communication, 2007; Petersen et al., submitted).


165

Widespread high-Ca and mafic granitoid magmatism in the Kambalda area

(Champion and Sheraton, 1997) accompanied compression, and led to the development

of skarn-type epidote-calcite-magnetite-pyrite-chalcopyrite-quartz alteration in mafic

rocks adjacent to intermediate porphyry stocks at Kambalda (Neumayr et al., 2004).

Mueller noted similar hydrothermal alteration associated with high-Mg monzodiorite-

tonalite intrusions at the Hannan South mine and Shea prospect, which he described as

Cu-Au endoskarns. He noted that biotite-sericite alteration and oxidized ore-related

mineral assemblages at Mt Shea were identical to magnetite-hematite bearing gold lodes

at Kambalda and the Golden Mile and considered that they formed due to oxidized

magmatic fluids ascending from buried subduction-related monzodiorite-tonalite

plutons. This style of skarn-type alteration and mineralization was not observed

associated with the ore-hosting M1 and M2 porphyry dikes at New Celebration.

5.3 D3 (2660-2647 Ma) -D4 (<2640 Ma) Deformation The onset of regional D3 deformation marked a change in the evolution of the

BLFZ from discrete thrust ramps to a continuous, crustal-scale strike-slip fault system

(Weinberg et al., 2005). This event was associated with the onset of significant gold

mineralization at New Celebration (Figs. 7.13 and 7.14) and Kambalda (Fig. 7.15).

Importantly, however, the D3 right and left-lateral and oblique reverse faults at the

Golden Mile are not associated with gold mineralization or significant hydrothermal

alteration and cut earlier Fimiston and Oroya lodes (Bateman and Hagemann, 2004).

Gold mineralization at New Celebration and Kambalda during D3 and early D4

took place in at least two stages; the first associated with ductile strike-slip deformation

on the BLFZ, and the second, associated with brittle-ductile reactivation of the BLFZ

and following a period of significant uplift and erosion. The first ductile deformation-

related mineralization event in the Kalgoorlie-Kambalda corridor was restricted to New

Celebration (Stage I Au, Fig 7.13) and involved the formation of gold mineralization

within ductile, oblique-slip, shear-related fabrics in magnetite-altered intermediate

plagioclase porphyry and mylonitized mafic schist (Nichols, 2003). The gold-bearing,

aqueous-carbonic fluids are characterized by low- to moderate salinity (2-7 wt.% NaCl

equiv.), low to medium XCO2 (0.03-0.3) and trace methane (XCH4 = 0.0-0.04), and had

K/Ca ratios of <1. Formation temperatures and pressures ranged between 330 and 500°

C and 2.4 and 4.2 kbars, respectively, which corresponds to crustal paleodepths between

10 and 14 kilometers (cf. Brown and Hagemann, 1995). Gold precipitated by wall rock

reaction between sulfur-bearing hydrothermal fluids and magnetite-bearing wall rocks.


166

The second brittle-ductile deformation-related Au event was observed at New

Celebration (Stage II Au, Fig. 7.14), Kambalda (Fig. 7.15) and Kalgoorlie (Mt Charlotte

Au, Fig. 7.16) gold camps. The reactivation of the BLFZ and associated hydrothermal

alteration and fluid flow controlled gold mineralization at New Celebration and

Kambalda and with right-lateral oblique slip faults at Kalgoorlie. There are significant

commonalities between the ore fluids at all camps. Gold mineralization at New

Celebration formed from a low salinity (3 to 7 wt.% NaCl equiv.) aqueous-carbonic

fluid with variable carbon dioxide contents (XCO2= 0.03 to 0.76), and Clark et al.

(1989) documented similar fluids (8 to 9 wt.% NaCl equiv. and XCO2=0.1 to 0.2)

associated with gold related metasomatism at the Victory deposit. Aqueous-carbonic,

low-salinity (2.0 to 5.5 equiv. wt. % NaCl) fluids characterized Mt Charlotte Gold

mineralization. Stage II gold mineralization at New Celebration occurred at

temperatures and pressures between 280 and 360° C, and 1 to 3.5 kbars, respectively

from a combination of: (1) phase immiscibility; and (2) wall rock sulfidation reactions

(this study), and possibly a fluid mixing component. Potassium/Ca ratios of the Stage II

ore fluids are greater than 1, which indicates that a switch in fluid source took place

between Stage I and Stage II gold mineralization at New Celebration. Clark et al. (1989)

proposed that gold mineralization at the Victory deposit was related to wall rock

metasomatic reactions at 390±40° C and 1.7 to 2.0 kbars. They concluded that gold

mineralization occurred at significantly lower temperatures and pressures than those

estimated for peak metamorphism (2.5 to 3.5 kbars and 450 to 570° C, (Archibald,

1985)) and, therefore, took place after a period of significant uplift and erosion.

In a recent, on-going, Kambalda camp-scale investigation on the hydrothermal

fluid flow and gold mineralization, Neumayr et al. (2004; 2008) and Petersen et al.

(2005) concluded that gold mineralization formed at zones of redox gradient due to the

influx of magmatic sulfate-bearing CO2-dominated (oxidized) fluids into the existing

reduced (CH4-N2±CO2) hydrothermal fluid system. They theorized that the oxidized

CO2-rich fluid entered the hydrothermal system via intermittent tapping of deeper

crustal CO2 reservoirs or CO2-rich magmas during fault movement (cf. Cox and

Ruming, 2004).

Charlotte-style sheeted quartz vein deposits (Ridley and Mengler, 2000;

Bateman and Hagemann, 2004) characterize gold mineralization associated with right-

lateral, oblique slip D4 faults. The type example is the Mt Charlotte deposit at the

northern end of the Kalgoorlie gold camp, but significant Charlotte-style mineralization


167

also occurs throughout the Golden Mile (Harbi, 1997; Bateman et al., 2001; Bateman

and Hagemann, 2004). Sheeted quartz-carbonate±scheelite veins in the granophyric

Unit 8 of the Golden Mile Dolerite in the footwall of closely-spaced D4 strike-slip faults

(Clark, 1980) characterize the Mt Charlotte deposit. Gold related hydrothermal

alteration adjacent to the veins is zoned both laterally and vertically, with albite, chlorite

and magnetite replacing ankerite, sericite, pyrite, siderite and rutile proximal to the

veins, and pyrrhotite progressively replacing pyrite with increasing depth (Clark, 1980;

Mikucki and Heinrich, 1993). Hydrothermal fluid chemistry varies slightly with depth,

but is characterized mainly by aqueous-carbonic, low-salinity (2.0 to 5.5 equiv. wt. %

NaCl) fluids. There is a distinct vertical gradient (Mernagh, 1996) in fluid temperature

(200-440° C), which corresponds with the changing alteration assemblages with depth.

The highest homogenization temperatures are observed in quartz veins at more than

800m depth below the present-day surface (Mernagh, 1996). The majority of the gold is

located within the wall rocks, and not within the veins, indicating that wall rock

sulfidation was the dominant ore forming process, although Mernagh (1996) proposed

cooling and oxidation of the ore-bearing fluid as it reacted with host rocks as an

alternative gold precipitation mechanism (Clark, 1980; Phillips, 1986; Ho et al., 1990).

Fluid inclusion evidence from Mt Charlotte (Clark, 1980; Ho et al., 1990) indicate that

phase separation was also a contributing factor to gold precipitation within the quartz

veins.

Movement along the BLFZ during the regional D4 deformation event is

contentious. At New Celebration, Nichols (2003) documented post-D3 horizontal

slickenlines on the BLFZ, indicating strike-slip movement of unknown direction and

displacement. At Kalgoorlie, there is no direct evidence for fault zone movement at the

BLFZ during regional D4 (Swager, 1989). Regional D4 at Kalgoorlie is expressed by a

series of north north-easterly striking dextral faults that offset all previous structures

(Swager, 1989; Bateman and Hagemann, 2004). The precise geometry of their

interaction with the BLFZ is not known. One possibility is that the oblique faults are

secondary features controlled by a reversal of shear direction, from sinistral to dextral,

along the pre-existing BLFZ. Evidence for this hypothesis is that the D4 Golden Pike

fault is deflected at its intersection with the BLFZ (Woodall, 1965). The observation

that the Golden Pike fault curves, for a considerable length, from an oblique to a strike

parallel orientation, is an argument in favor of this shear reversal. Alternatively, the D4

oblique dextral faults are unrelated to the BLFZ.


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The D3 and D4 events saw the establishment of the BLFZ as a single cohesive

fault on a regional scale, and the introduction of widespread gold mineralization

throughout the Kalgoorlie-Kambalda corridor. Mineralogical and geochemical evidence

indicates that this episode of gold mineralization was unrelated to formation of the

earlier Fimiston and Oroya lodes. The New Celebration and St Ives deposits are

unequivocally linked to the western segment and the Lefroy segment of the BLFZ,

respectively, however, the relationship between gold at Mt Charlotte and the BLFZ is

less certain. It is likely that gold at the Mt Charlotte deposit formed from the same

crustal fluid reservoir as New Celebration and St Ives, however, hydrothermal fluid

movement at the latter two was focused via the BLFZ, whereas the hydrothermal fluids

that formed Mt Charlotte Au exploited the same (and as yet unidentified?) regional

crustal structures that facilitated Fimiston and Oroya mineralization.

5.4 Post-D4 There is presently no evidence for post-D4 structures, or deformation along the

BLFZ in the Kalgoorlie-Kambalda corridor, other than east-west trending Proterozoic

dikes


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Figure 7.10 Schematic representation of Fimiston -style gold mineralization during D1 at the Golden Mile camp. A. Cross-section of the Kalgoorlie anticline and Golden Mile fault

at a regional scale showing fluid flow up a crustal scale rift fault and along the Golden Mile fault where gold precipitates through phase immiscibility (high/bonanza grade gold in

open space fill veins and breccias) and wall rock reaction (low grade disseminated halo). Potential fluid sources are shown. Figure A from Bateman and Hagemann, 2004. B.

Enlargement of the rectangle in A emphasizing the processes and textures leading to and resulting from gold mineralization.


170

Figure 7.11 Schematic representation of Oroya -style gold mineralization during D2 at the Golden Mile camp. A. Cross-section of the Kalgoorlie anticline and Golden Mile fault at a

regional scale reoriented and tilted upright during regional E-W deformation. From Bateman and Hagemann, 2004. B Schematic representation of ore textures and distribution of

high and low grade zones in Oroya lodes.


171

Figure 7.12 A. Schematic cross-section through the New Celebration gold deposit showing potential fluid and metal sources and the location of gold mineralization during the

formation of Stage I gold mineralization and D3NC deformation. B. Enlargement of oblong in A illustrating the ore forming processes and the distribution of mineralization adjacent

to the BLFZ.


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Figure 7.13 A. Schemstic cross section through the New Celebration gold deposit after the emplacement of the M2 felsic porphyry dyke and during Stage II gold mineralization,

during late D3 or early D4. B. Enlargement of oblong in A illustrating the ore forming processes and location of gold mineralization with respect to the dyke .


173

Figure 7.14 A. Schematic cross section through the St Ives gold camp showing the relationship of gold mineralization to the BLFZ and the second order Playa fault. B. Location of

gold mineralization and gold precipitation mechanisms. Fig. B from Nguyen et al. 1998


174

Figure 7.15 A. Location of Mt Charlotte style gold mineralization with respect to the BLFZ and to right-lateral D4 strike-slip faults. B. Schematic diagram of high and low grade

zones within Unit 8 of the Golden Mile Dolerite. Fig. B modified from Bateman and Hagemann, 2004


175

that intruded tensional fractures. Williams (1994) and Nichols (2003) observed quartz-

calcite-chlorite veins that crosscut D3 foliation, gold mineralization and post-D3NC

slickenline orientations, which Nichols (2003) assigned to D4NC. In addition, various

workers throughout the Kalgoorlie-Kambalda corridor observed fluid inclusion trails

that crosscut earlier gold-related quartz crystals and associated fluid inclusion

assemblages, suggesting significant hydrothermal fluid circulation after the cessation of

gold mineralization throughout the region. Unfortunately, in most studies, these fluid

inclusion trails cannot be correlated with deformation events; therefore, they remain

temporally unconstrained.

Widespread high salinity (18-37 wt.% NaCl equiv.) aqueous fluids, trapped as

secondary fluid inclusions in trails that crosscut quartz grain boundaries, are reported

from New Celebration (Hodge et al., in revision) and Kambalda (Clark et al., 1989). At

New Celebration, Hodge et al. (in revision) calculated minimum formation temperatures

and pressures of 100 °C-180 °C and 0.4 to 1 kbar, indicating that these fluids were

trapped at significantly higher crustal levels than the ore forming fluids. They

considered that these fluids were likely unrelated to the ore fluids, and were well after

mineralization took place, and after a period of uplift and erosion. Potassium-calcium

ratios and trace element compositions indicate a potential magmatic source for these

fluids. In contrast, Clark et al. (1989) interpreted these secondary fluid inclusions at

Kambalda to be the consequence of phase separation of the earlier moderately saline

CO2-bearing fluids during the late stages of mineralization (cf. Robert and Kelly, 1987).

It is worth noting that Bouiller et al. (1998), in their work on lode gold deposits of the

Archean Abitibi belt, disproved Robert and Kelly's (1987) work on the Sigma mine and

demonstrated that the saline inclusions were unrelated to gold mineralization and were

likely crustal shield brines. It is possible that Clark et al's (1989) interpretation of the

saline inclusions at Kambalda is also incorrect, and that they post-date mineralization

and are related to similar inclusions at New Celebration. At New Celebration, the latest

observed fluid inclusion assemblages contain predominantly methane, with minor

ethane (C2H6) and propane (C3H8), and, are interpreted as the latest stage fluid

circulating within the BLFZ. The timing of these fluids is again unconstrained; they

may have been introduced immediately after gold mineralization and by implication

when the BLFZ potentially was connected to the mantle, or millions of years later. At

New


176

Figure 7.16 Timing chart summarizing the geological, deformational and mineralization history of the Kalgoorlie-Kambalda corridor


177

Celebration, it is noteworthy that these reduced methane-rich fluids characterize the first

and last observed fluid events (Hodge et al. in revision).

6. DISCUSSION

The giant Golden Mile and world-class New Celebration and St Ives deposits,

all spatially associated with the BLFZ, show a number of similarities with regard to

their mineralogy and hydrothermal fluids. They are: (1) at all deposits, the ore-forming

fluids are low to moderate salinity (<1 to ~15 wt.% NaCl equiv.) mixed aqueous-

carbonic (XCO2 = 0.03-0.3 but locally up to 1.0) fluids with minor methane (XCH4=0.0

to 0.04); (2) the dominant ore-forming mechanism at each deposit is wall rock reaction

between gold and sulfur bearing ore fluids and Fe-oxides, and (3) gold mineralization at

all camps is accompanied by broadly similar hydrothermal alteration mineralogy, such

as ankerite, siderite, albite and pyrite. However, there are a number of discrepancies

evident between the different deposits.

6.1 Geochemistry Geochemically, there are a number of significant differences between the

Fimiston and Oroya lodes at the Golden Mile, and all other gold mineralization in the

corridor. These are: (1) the Fimiston and Oroya styles of gold mineralization at the

Golden Mile are associated with vanadian-rich minerals, which are not observed

elsewhere in the Kalgoorlie-Kambalda corridor; (2) gold mineralization at the Golden

Mile is commonly associated with extensive telluride mineralization not observed

elsewhere in the corridor; and (3) a number of textural and fluid characteristics at the

Golden Mile suggest mineralization took place at much shallower crustal levels than at

New Celebration or St Ives.

Results of this study have further differentiated Fimiston and Oroya lodes from

other gold mineralization in the corridor on the basis of their sulfide geochemistry,

which distinguished these lodes from the New Celebration and St Ives deposits by their

high As and Sb concentrations, and extremely high Te concentrations in pyrite, which

are orders of magnitude higher than those measured in New Celebration and St Ives

pyrites. These aspects of the detailed evolution of the BLFZ and associated gold

mineralization warrant further discussion.

(1) The Fimiston and Oroya lodes contain V associated with the ore fluid,

evidenced by the presence of V-rich muscovite (roscoelite), which is not reported from


178

either New Celebration or Kambalda. Roscoelite is rare in mesothermal lode gold

deposits, however it is a relatively common in epithermal gold-telluride deposits (e.g.

Cripple Creek, Colorado: (Jensen and Barton, 2000); Emperor, Fiji: (Ahmad et al.,

1987b); and Porgera, Papua New Guinea: (Cameron et al., 1995; Cameron, 1998))

where the presence of vanadium is usually linked to alkalic igneous rocks spatially

related to the gold deposits (e.g. Ahmad et al., 1987b; Zhang and Spry, 1994; Pals and

Spry, 2003).

(2) The Fimiston and Oroya lodes contain nineteen identified tellurides

(Shackleton et al., 2003 and references therein) and Te concentrations in Fimiston and

Oroya pyrites range up to 2400 ppm. Thermodynamic modeling predicts Te

transportation in magmatic hydrothermal vapors (Cooke and McPhail, 2001) therefore,

the high Te concentrations reported at the Golden Mile imply a magmatic fluid source.

(3) A number of features of the Golden Mile Fimiston and Oroya deposits

suggest formation at significantly shallower crustal levels (<~6km) than other deposits

in the region. There is a high abundance of open space-fill ore textures at the Golden

Mile that are not observed anywhere else in the Kalgoorlie-Kambalda corridor.

(4) New evidence from this study reveals high As and Sb concentrations in

Fimiston and Oroya ore-stage pyrites. This supports a magmatic fluid source for these

lodes, and the presence of Sb in Fimiston and Oroya pyrites suggests emplacement of

these lodes at epizonal crustal levels and at temperatures <300° C (Pitcairn et al., 2006).

6.2 Timing There are also a number of timing issues surrounding the formation of gold

mineralization in the Kalgoorlie-Kambalda corridor and its relationship to the BLFZ.

The early timing of Fimiston and Oroya mineralization at the Golden Mile and the

potential absence during these mineralization events of a coherent BLFZ appears to

preclude the BLFZ as a feeder zone for hydrothermal fluid migration and suggests that

mineralization at the Golden Mile is unrelated to the BLFZ, and other deposits in the

corridor. Seismic interpretations on the nature of the crust beneath the Golden Mile

indicate that the BLFZ dips to the west in this area (Goleby et al., 2002). This would

place the Golden Mile deposit in the footwall of the BLFZ, and there is no structural

evidence to suggest that the Golden Mile was ever linked to the BLFZ. A new study on

the structural architecture of the St Ives deposits by Miller et al. (2009) indicates that at

Kambalda, the Lefroy segment of the BLFZ exploited structures formed during rifting


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and emplacement of the mafic-ultramafic volcanic sequence, during De extension. At St

Ives, the BLFZ is in fact an east-dipping, partially inverted normal fault and not a west-

dipping thrust fault as it is interpreted further to the north. It is likely that similar relict

rift architecture provided the hydrothermal fluid pathways at Kalgoorlie during Fimiston

and Oroya gold mineralization as the orogen switched from an extensional to a

compressional regime.

Traditional models for orogenic lode gold deposits constrain the timing of

mineralization to late in the tectonic evolution of the host terrane (Colvine et al., 1988;

Groves et al., 1989; Hodgson, 1993; McCuaig and Kerrich, 1998). Greenschist-facies

hosted gold deposits typically post-date the regional metamorphic peak and have

hydrothermal alteration assemblages that are retrograde with respect to the metamorphic

assemblages. Phillips (1986) interpreted the chlorite-carbonate assemblage at the

Golden Mile as coeval with gold mineralization and that it replaced the regional

metamorphic assemblage. In contrast Gauthier et al. (2004; in revision) document

regional NNW trending foliation overprinting Fimiston-style lodes, indicating that the

lodes were emplaced prior to regional compression and peak metamorphism.

Swager (1989) considered the development of the BLFZ crustal wrench fault

during D3 as a critical component in focusing auriferous fluids to the region, and that it

was the locus for gold deposition from Kalgoorlie to Kambalda. However, the D3

deformation event, which is associated with the main gold mineralizing stages at New

Celebration and Kambalda, is barren at Kalgoorlie. Weinberg et al. (2005) considered

that the BLFZ developed in two main stages – an early stage that resulted from east-

west compression and crustal thickening during D2, and which formed a number of

discrete north-northwest-trending, east- and west-dipping thrust ramps linked by

transfer faults, and a second stage of sinistral reactivation during D3, which led to the

linking of the thrust planes and the formation of a single, regionally extensive shear

system. It is also unclear exactly how the Boulder and Lefroy segments of the fault link

together at depth. The change in orientation observed between St Ives and New

Celebration cannot be accounted for by a simple single-strand fault system; therefore,

further studies to elucidate the nature of the crustal architecture north of Kambalda

could provide an answer. No current interpretation of the fault kinematics, however,

allows for the existence of the BLFZ as a regionally extensive, crustal scale structure

during the early formation of the Golden Mile Fimiston- and Oroya lodes – combined

these are the largest gold deposit in the Yilgarn craton – during D1 and early D2. There


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are three alternatives to explain this (1) the BLFZ was active much earlier than

previously interpreted, at least during D1; (2) gold mineralization at the Golden Mile

was in fact late in the tectonic evolution of the terrane and the interpretations of D1

mineralization by Bateman et al. (2001) and Bateman and Hagemann (2004) are

erroneous; or (3) Golden Mile mineralization is unrelated to the BLFZ.

(1) Gee (1981) considered that the deep crustal scale faults in the Yilgarn

originated during extension as feeder faults for early volcanism., There is no evidence at

Kalgoorlie or New Celebration for the existence of, or movement along, the BLFZ

during D1, however, a recent study by Miller et al. (2009) which used seismic profiles

and dolerite thickness isopachs at St Ives to delineate the underlying structures indicates

that at least at St Ives, the original rift architecture had a strong influence on the

formation of crustal structures during post-extensional compression, and that a proto-

BLFZ was in place at Kambalda at least during D1 and likely during De. Similar

detailed investigations have not yet been carried out in the Kalgoorlie or New

Celebration areas, but there is currently no evidence for pre-D2 movement on the BLFZ

at either of these localities (Nichols, 2003; Weinberg et al., 2005; Nichols et al., in

revision). Option 2 is considered unlikely. Recent age determinations by Gauthier et al.

(2004) and Gauthier et al. (submitted) support the detailed structural studies carried out

by a number of authors (Bailly et al., 2000; Bateman et al., 2001; Bateman and

Hagemann, 2004) who consider that mineralization at the Golden Mile occurred early in

the tectonic evolution of the belt. This interpretation is consistent with the recent work

of Morey (2007), who evaluated gold mineralization and structural controls within the

Bardoc Tectonic Zone (BTZ), immediately to the north of Kalgoorlie. He concluded

that mineralization along the BTZ was associated with early D2 E-W compressional

tectonics and that the D3 strike-slip event was insignificant. Further, seismic evidence

for a west-dipping BLFZ in Kalgoorlie (Goleby et al., 2002) places the Golden Mile in

the footwall of the fault, which would be unlikely if the BLFZ was actually related to

Golden Mile gold mineralization. If we accept that Fimiston mineralization at the

Golden Mile took place early in the deformational history of the terrane then it was not

associated with the BLFZ. The evidence from this study, in conjunction with recent

work done on the Golden Mile and Kambalda deposits, suggest that option three is most

likely i.e. gold mineralization at the Golden Mile is unrelated to either the BLFZ, or to

gold mineralization at New Celebration or Kambalda.


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In contrast, there is abundant evidence that the New Celebration and St Ives

deposits are related to each other and to the BLFZ. Gold mineralization at both areas

took place later in the orogen, when the BLFZ was established as a cohesive, single,

crustal scale shear zone (Weinberg et al., 2005). Both deposits show a direct connection

with the BLFZ – New Celebration gold mineralization is hosted directly within the

western segment of the fault and the St Ives deposit formed within the Playa fault – a

second order splay in the footwall of the BLFZ. Stage I gold mineralization at New

Celebration is hosted in pyrite, which is in textural equilibrium with S3 foliation planes

(Nichols, 2003), and Stage II gold mineralization is hosted within a boudinaged felsic

porphyry emplaced directly into the fault (Norris, 1990; Copeland, 1998). Both the New

Celebration and St Ives deposits show fluid inclusion evidence for methane within the

hydrothermal system, consistent with the development of the hydrothermal system in an

environment with a mantle connection, evidenced by the presence of lamprophyres

contemporaneous with gold mineralization at both camps (cf. Rock and Groves, 1988a;

Rock, 1990).

7. CONCLUSIONS

Recent work on the Kalgoorlie-Kambalda corridor challenges the traditionally

held interpretations that the gold deposits of the region are temporally and genetically

related to each other and to the BLFZ. If we accept that Fimiston- and Oroya-style gold

mineralization at the Golden Mile took place during D1 and D2, and predated peak

metamorphism (cf. Gauthier et al., 2004), then the widely accepted metamorphic

devolatilization model (Phillips et al., 1987) used to explain the source of hydrothermal

fluids and metals including gold has to be called in to question. Clout (1989) proposed a

significant surface water component to the Fimiston and Oroya lodes and, based on

oxygen, hydrogen and sulfur isotopes, and in conjunction with the textural features,

classified the Golden Mile as a near-surface epithermal Au-Te deposit. The presence of

vanadium in roscoelite, extremely rare in mesozonal orogenic gold deposits, but

characteristic of low sulfidation epithermal Au-Te deposits, suggests an alkalic

magmatic origin for the Golden Mile. Bateman et al. (2001) related gold mineralization

to east-over-west thrusts on the Golden Mile fault, and it is possible that this fault

tapped a magmatic fluid reservoir, which led to the formation of the Golden Mile

deposits in a shallow crustal, epizonal environment prior to the development of the

crustal scale BLFZ. A magmatic origin for the Golden Mile is consistent with the

interpretations of Bateman et al. (2001), who concluded that the sulfur isotopic


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compositions of sulfides from the Oroya-style lode were consistent with mixing an

oxidized magmatic fluid with heavy sulfur-bearing metasedimentary units within the

Paringa Basalt, and with Clout (1989) who postulated a shallow epithermal origin for

the Golden Mile deposit based on the open space ore textures and oxygen isotopes of

gold-related quartz veins, which indicated a meteoric water component to the ore fluid.

Gauthier et al. (in revision) also postulated a magmatic association, based on the

contemporaneity of Fimiston-style lodes with intermineral andesite dikes.

Increased methane contents ore fluids from Oroya-style lodes, which formed

during early D2, may reflect the onset of faulting along the BLFZ trend, which

introduced deep crustal or mantle methane into the hydrothermal fluid system. Ductile

and brittle-ductile related gold mineralization at New Celebration and Kambalda,

associated with D3 sinistral strike-slip and oblique-slip movement on the BLFZ was

related to the formation of, and deformation along, the BLFZ and reflects separate

processes and fluid sources to the Golden Mile deposits. The results of this study, and

evidence from other researchers (Hagemann et al., 1999; Bateman et al., 2001; Nichols,

2003; Bateman and Hagemann, 2004; Gauthier et al., 2004; Neumayr et al., 2004;

Petersen et al., 2005; Petersen et al., 2006; Walshe et al., 2006; Neumayr et al., 2008;

Miller et al., 2009; Gauthier et al., in revision) leads to the following conclusions:

1. Fimiston and Oroya style gold mineralization took place at the Golden Mile prior

to regional peak metamorphism and the formation of the BLFZ. It is unrelated to

the fault, or to either the New Celebration or Kambalda deposits, and likely

formed from magmatic fluid and/or metal sources in a shallow crustal

environment.

2. The New Celebration and Kambalda deposits show a number of similarities,

including fluid chemistry, alteration mineralogy, and sulfide composition. They

appear to be genetically related, i.e. they formed during the same D3 deformation

event and the hydrothermal fluids for each deposit were likely sourced from the

same crustal fluid reservoirs and transported via the BLFZ and its higher order

splays

3. The Golden Mile deposit, which is one of the largest in the world, is unique and

distinctive to the region and is unrelated to the BLFZ.

If the Golden Mile deposit is unrelated to the BLFZ, the question remains, what

then, facilitated the movement of such immense volumes of hydrothermal fluid into an


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area that generated one of the world’s richest gold deposits? Evidence from Kambalda

that indicates that syn-mineralization structures exploited a crustal architecture

established as much as 70 million years earlier might provide the answer. The

Kalgoorlie gold deposits formed during the change from extension, accompanied by

mafic-ultramafic and bimodal mafic-felsic volcanism, to compression. At this point, the

deep crustal rift structures would still have been connected to the deep crust and upper

mantle, and could have provided the hydrothermal fluid pathways that facilitated the

movement of magmatic fluids, enriched in gold, tellurium and vanadium, to the upper

crust, which provided ideal physico-chemical conditions for the formation of the giant

Golden Mile deposit. This structure has yet to be identified in the Kalgoorlie region, but

could lie along the eastern margin of the current Kalgoorlie camp.

ACKNOWLEDGEMENTS

This paper was conceived and written during the first author’s PhD research at

the University of Western Australia. The first author (JLH) acknowledges the support of

an Australian Postgraduate Award and a pmd*CRC supplementary scholarship. The

pmd*CRC is also thanked for providing research funding, and Dr R. Hayden (CEO) is

thanked for permission to publish. Analytical facilities were provided by the University

of Tasmania, and particular thanks go to Sarah Gilbert, for assistance with LA-ICP-MS

mineral chemistry analyses, and Garry Davidson and Keith Harris for sulfur isotope

analyses

CHAPTER EIGHT: CONCLUSIONS

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8 CHAPTER EIGHT: CONCLUSIONS The Boulder-Lefroy fault zone is spatially correlated with one giant (>1000 t

Au) and two world-class (>100 t Au) gold deposits, in addition to a number of smaller

deposits, which together have produced in excess of 2000 t of gold since it was first

discovered in 1893. The relationship between major crustal breaks and orogenic gold

deposits has long been recognized, however, the first-order segments of these fault

systems are in general poorly researched, mostly due to a lack of exposure, but also

because most gold endowment is contained in higher order splays, and not within the

first order segments themselves. The New Celebration gold deposit, which exposes the

BLFZ in the open pit, provides a unique opportunity not only to study a major crustal

break located in one of the world’s most richly gold endowed corridors, but also to

study a world-class deposit located directly within the fault.

The major objectives of this thesis were to: (1) document the pressure-

temperature-composition characteristics of the mineralizing and non-mineralizing

hydrothermal fluids in the BLFZ at New Celebration, (2) determine the metal content of

gold-bearing and barren fluids within the New Celebration hydrothermal system, (3)

characterize the major and trace element composition of hydrothermal oxides, ore-stage

sulfides and gold, and the sulfur isotopic composition of ore-stage pyrites, (4) to

critically evaluate these datasets with a view to evaluating the potential source (or

sources) of these fluids, and (5) integrate all the available data into a hydrothermal fluid

model for the evolution of the BLFZ and related gold mineralization at New

Celebration. An additional aim was to compare and contrast the three major gold camps

(Golden Mile, New Celebration, St Ives) of the Kalgoorlie-Kambalda corridor in terms

of their geochemistry, hydrothermal alteration, stable isotopic signatures and

mineralization styles, and evaluate the role of the BLFZ in forming one of the richest

gold mineralized corridors on earth.

8.1 New Celebration Hydrothermal Fluid System

Petrographic, fluid inclusion and isotopic analyses of the pre- and syn-gold

related veins and ore-related host sulfides at New Celebration indicate that: (1) the two

stages of gold mineralization at New Celebration formed from differing hydrothermal

fluids from different processes under differing P-T conditions during the evolution of

the Boulder-Lefroy fault zone, and (2) the BLFZ was the conduit for a variety of fluids


185

at different times during its evolution and had a protracted (mid D3 to D4, ~ 20 million

years) and complex fluid history.

8.1.1 Gold Mineralization

Aqueous-carbonic fluid inclusions trapped in syn-D3NC type 2 quartz-carbonate

veins indicate that Stage I gold mineralization took place at temperatures between 330

°C and 390 °C and between 3.2 and 4.0 kbars at a crustal depth between 10 and 15

kilometers (assuming lithostatic fluid pressures) during ductile deformation. The ore-

forming fluids were H2O-CO2 dominant, with salinities between 1.9 ± 1.2 and 5.9 ± 0.7

wt. percent NaCl equiv. They contained 10 ±1 to 33 ± 13 mole percent CO2 and up to

33 ± 1 mole percent CH4. Gold precipitated as a consequence of sulfidation reactions

with iron-rich wall rocks in which pre-existing hydrothermal magnetite alteration

provided sufficient iron to facilitate gold precipitation by wall rock sulfidation in an

otherwise iron-poor host rock. There was no fluid inclusion evidence for phase

separation or fluid mixing during Stage I gold mineralization.

Stage II mineralization, as evidenced by aqueous and aqueous-carbonic

inclusions trapped in post-D3NC type 3 quartz veins, formed at temperatures (between

280 °C and 320 °C) and pressures (between 0.8 and 3.2kbar), corresponding to crustal

depths between 4 and 10 kilometers (assuming lithostatic fluid pressures) during brittle-

ductile deformation. Stage II hydrothermal fluids were H2O-CO2 dominant, with

calculated salinities between 3.6 ± 0.3 and 5.7 ± 1.0 wt. percent NaCl equiv. and

between 16 ± 3 and 76 mole % CO2. Sulfidation reactions between sulfur-bearing gold-

rich fluids and iron oxides in high magnesium basalt facilitated gold precipitation for

Contact-style mineralization along the contacts of the M2 felsic porphyry dike. The

presence of liquid-rich and vapor-rich end member fluid inclusions, total

homogenization into liquid and vapor at the same temperature and variable bulk

compositions and molar volumes of inclusions within individual trails or clusters in type

3 quartz veins, and the lack of petrographic evidence for wall rock sulfidation in the M2

porphyry dike indicate that phase separation was the likely cause of gold precipitation in

Fracture-style mineralization. Vapor-rich carbonic inclusions, observed in type 3 quartz

veins, indicate the presence of a CO2-rich fluid at some point in the hydrothermal

evolution of New Celebration. The paragenetic relationship between these CO2-rich

inclusions and the gold-bearing aqueous-carbonic inclusions are unclear, due to a lack

of observed cross-cutting relationships, however, their presence in the system suggests


186

that there may have been a degree of fluid mixing between gas-rich and gold bearing

fluids during the evolution of the hydrothermal system.

Laser ablation-ICP-MS analyses on individual fluid inclusions revealed that

gold-related aqueous carbonic fluid inclusions contained up to 51ppm Au and

significant concentrations of other metals such as Cu, Pb and Zn. The H2O-CO2

inclusions in type 2 veins were Na-Ca dominant, with subordinate K and Mg, and had

K/Ca ratios <1. Individual fluid inclusions contained up to 51ppm gold although

average concentrations were around 5ppm (n=80). Concentrations of other metals were

generally low, although these inclusions did contain up to 163ppm Cu, 75ppm Zn and

43ppm As. The H2O-CO2 inclusions in type 3 veins and quartz alteration associated

with Contact style mineralization contained higher Na, Mg and K concentrations, but

lower Ca (K/Ca >1) than those in type 2 veins. Stage II fluids had up to 33ppm Au

(n=60), and generally contained higher concentrations of Cu, Pb, Zn, Sr, As, Sb, Bi, Sn,

Mn and Fe than fluids associated with Stage I gold mineralization.

The change in K/Ca ratios and variable metal concentrations from Stage I to

Stage II indicate that a switch in fluid source occurred between Stage I and Stage II

mineralization. The source of both the metals and fluids is currently unconstrained;

however, the change in fluid characteristics from a Na-Ca dominated fluid to a Na-K

dominated fluid possibly represents a switch from metamorphic fluids, derived from the

devolatilization of deep crustal rocks undergoing regional scale metamorphism, to fluids

of magmatic origin, coinciding with the emplacement of the M2 porphyries.

The sulfur isotopic composition of ore-stage pyrites also illustrated differences

between the two mineralizing events, and reinforced the interpretation that

mineralization at New Celebration took place by different processes and from different

fluid sources. Stage I pyrites had 34S values between -7.6 and +3.8 per mil, whereas

Stage II pyrites had more negative values, between -10.6 and -3.2 per mil. These values

are generally more negative than typically reported from orogenic lode gold deposits in

both Australia and Canada (McCuaig and Kerrich, 1998). The isotopic composition of

Stage I pyrites is interpreted to reflect the sulfur composition of the ore fluid, as the

replacement of wall rock magnetite by pyrite will not result in in situ fluid oxidation

during gold precipitation (Palin and Xu, 2000). Fluid inclusion evidence indicates that

Stage II mineralization formed at least partially due to phase immiscibility. This process

does lead to fluid oxidation (Drummond and Ohmoto, 1985) and depletion of 34S in the


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residual liquid and partially accounts for the negative values to -10.6 per mil and the

spread of values between -10.6 and -3.2 per mil observed in Stage II ore-related pyrites.

Trace element analyses of sulfides and oxides revealed that pyrites from Stage II

Fracture-style mineralization showed markedly different trace element patterns than

those pyrites related to both Stage I mineralization styles and Stage II Contact-style

mineralization. They showed depletion of Ni, Co, Mn, Cr, and Zn but enrichment of Pb

and Bi relative to Stage I and Stage II Contact-style pyrites, and a far higher proportion

of poly-metallic inclusions within the pyrite grain compared to Stage I and Stage II

Contact style pyrites. This likely reflects the differing ore-forming processes and fluid

sources between the mineralization styles and stages where Stage I and Stage II Contact

style pyrites reflect the composition of wall rock magnetites from which the pyrites

formed whereas the composition of Stage II pyrites reflects fluid composition

8.1.2 Hydrothermal Evolution

Pressures and temperatures calculated from all fluid inclusion types analyzed at

New Celebration, and independent geothermobarometric constraints, such as chlorite

geothermometry and phengite geobarometry (Williams, 1994), describe an

anticlockwise P-T path. These data, in conjunction with sulfur isotopic and major and

trace element compositions of ore-stage pyrites, and the trace element composition of

auriferous and barren hydrothermal fluids, as determined by single fluid inclusion

analyses, point towards a complex hydrothermal fluid system within the western

segment of the BLFZ. The two gold mineralizing stages were separated by a period of

uplift and erosion, and secondary post-gold fluid inclusions in types 2 and 3 quartz

veins record at least three distinct phases of fault zone reactivation at New Celebration.

High salinity aqueous inclusions, which are interpreted to post-date all other inclusion

populations except the latest methane inclusions, have pressure and temperature

trapping estimates that are significantly lower than for all previous fluid inclusion

assemblages (100° -180 °C, 0.4-1.0 kbars), suggesting significant uplift and erosion

during the final reactivation stages of the BLFZ.

The hydrothermal evolution of the BLFZ and New Celebration gold deposits is

characterized by discrete pulses of gold-bearing and barren hydrothermal fluids

infiltrating the fault as a consequence of distinct deformation events (D3NC to D4+NC)

including several reactivation events. At least two gas-rich fluid events are recorded that

cannot be linked to gold mineralization. The gold mineralization stages are


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characterized by aqueous-carbonic inclusions and as such are similar to many other

gold-bearing fluids observed in many orogenic gold deposits worldwide (cf. Phillips

and Groves, 1983; Wood et al., 1986; Robert and Kelly, 1987; Colvine, 1989; Groves et

al., 1989; Ho et al., 1990; Groves et al., 1992; Ho et al., 1992; Groves, 1993; Groves

and Foster, 1993; Hodgson, 1993; Mikucki and Ridley, 1993; Hagemann and Cassidy,

2000; Ridley and Diamond, 2000). Cation ratios indicate a fluid source switch between

Stage I and Stage II fluids. There is no fluid inclusion evidence for significant surface

water infiltration into the BLFZ at New Celebration (cf. Hagemann et al., 1993),

therefore, the switch in K/Ca ratios may relate to a change in deep fluid sources such as

magmatic or metamorphic fluids or a combination of the two. Methane-rich fluids are

evident throughout the evolution of the New Celebration hydrothermal system, and in

the absence of any outcropping black shales in the New Celebration deposit area, or

evidence for post-entrapment modification of fluid inclusions, or for Fischer-Tropsch-

type synthesis in reducing conditions, are interpreted to indicate mantle contributions.

8.2 Regional Hydrothermal Fluid System

The results of this study on the nature of the fluids in the BLFZ at New

Celebration and the new data on sulfur isotopic and geochemical composition of

sulfides from the Golden Mile, New Celebration and St Ives, in conjunction with

evidence from other researchers (Hagemann et al., 1999; Bateman et al., 2001; Nichols,

2003; Bateman and Hagemann, 2004; Gauthier et al., 2004; Neumayr et al., 2004;

Petersen et al., 2005; Petersen et al., 2006; Walshe et al., 2006; Neumayr et al., 2008;

Gauthier et al., in revision) challenge the traditionally held interpretations that the gold

deposits of the region are temporally and genetically related to each other and to the

BLFZ.

The Golden Mile is distinctive from other deposits in the Kalgoorlie-Kambalda

corridor, particularly in terms of its geochemistry and ore-related alteration

assemblages, but also in its relative timing to the formation of the orogen, the

development of the BLFZ as a cohesive fault system, and the timing of gold formation

at other centers in the corridor. The characteristic vanadian mica associated with the

Fimiston and Oroya lodes, and the abundance of telluride mineralization that formed

with gold, differentiate them from all other gold deposit styles in the Kalgoorlie-

Kambalda corridor. These features are more common in deposits that are spatially

related to alkalic igneous rocks and therefore imply a significant magmatic fluid


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contribution to the Fimiston and Oroya lodes. Antimony-rich ore-stage pyrites, which

are not observed at deposits elsewhere in the corridor, indicate formation temperatures

for the Fimiston and Oroya lodes of less than 300 °C, and in conjunction with open

space fill textures reported from these lodes, imply a low P-T epizonal setting for their

formation. Recent work by Bateman et al. (2001), Bateman and Hagemann (2004) and

Gauthier et al. (2004; in revision) indicates that the Fimiston and Oroya lodes at the

Golden Mile formed much earlier than originally proposed, prior to peak

metamorphism, during regional D1/D2. Recent work by Miller et al. (2009) at the St

Ives deposit, has postulated an early timing for the formation of the BLFZ in Kambalda,

perhaps as early as De, and consider that it reflects the underlying rift architecture active

during extension-related bimodal volcanism. Weinberg et al. (2005), however, indicated

that the BLFZ as a regional crustal scale structure did not exist prior to D2, and there is

no evidence for movement of the BLFZ during D1 or D2 at either Kalgoorlie or New

Celebration. Given the location of the Fimiston and Oroya lodes in the footwall of the

BLFZ, the lack of structural connectivity between the lodes and the fault, and the

apparent absence of an active BLFZ in the Golden Mile during the period that gold

mineralization took place, it therefore seems unlikely that gold mineralization is related

to deformation or fluid flow along the BLFZ. It is more likely that the hydrothermal

fluids, which formed the richest square mile on earth, exploited an existing underlying

crustal architecture emplaced during rifting, such as that observed at Kambalda (Miller

et al., 2009) but located somewhere to the east of the BLFZ and as yet unidentified.

In contrast, the New Celebration and Kambalda deposits show a number of

similarities to each other, including fluid chemistry, alteration mineralogy, and sulfide

composition, and appear to be unequivocally related to the BLFZ. St Ives gold

mineralization is located within the Playa fault, a second-order splay in the footwall of

the BLFZ, and the New Celebration deposit is located directly within the fault, either in

S3NC foliation planes or in boudinaged felsic porphyry. Mineralization at both deposits

formed late in the development of the orogen, when the BLFZ was a single cohesive

fault system, and both show direct connections to the BLFZ. Both show an abundance

of lamprophyres and methane-rich fluids inclusions, suggesting direct connectivity to

the mantle at some point (cf. Rock and Groves, 1988a, b; Rock et al., 1989).


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8.3 Exploration Implications

Although the role of crustal scale faults as vectors towards lode gold

mineralization in higher order structures has long been recognized (e.g. Eisenlohr et al.,

1989), crustal scale faults have been largely ignored as primary exploration targets.

Historically, most lode gold deposits have been discovered in higher order splays, which

are considered more advantageous sites for gold deposition due to their geological

complexity (Hodkiewicz, 2003), favorable dilational characteristics (Eisenlohr et al.,

1989; Groves et al., 1989; Kerrich, 1989; Robert, 1990) and localization of gold-bearing

ore fluids (Neumayr and Hagemann, 2002).

Gold mineralization at New Celebration clearly relates to the influx of gold-

bearing CO2-rich fluids into the western segment of the Boulder-Lefroy crustal-scale

fault zone during D3NC and D4NC deformation, where gold precipitated due to the

reaction of the hydrothermal fluids with magnetite-bearing intermediate and felsic wall

rocks (Stage I) and phase separation (Stage II). The New Celebration deposits are not

typical orogenic lode gold deposits in that they are hosted within a primary crustal scale

structure within predominantly intermediate and felsic intrusive rocks; a geological

setting mostly considered unfavorable for exploration in the Yilgarn Craton, where

mafic rocks host the majority of orogenic lode gold deposits (Groves, 1990). This study

illustrates that first-order fault systems do have the potential to host significant gold

mineralization where the physico-chemical parameters are favorable and should be

evaluated when exploring in both brownfields and greenfields terrains.

8.4 Future Work

This study provided better constraints on the metal composition of orogenic lode

gold fluids and demonstrates that a switch in fluid source took place between Stage I

and Stage II mineralization at New Celebration, however, the source (or sources) of the

mineralizing, and other, fluids within the hydrothermal system are still poorly

understood. Stable isotopic tracers do not unequivocally differentiate between source,

however, crustal reservoirs (mantle, magmatic, metamorphic) have unique noble gas

and halogen concentrations, which do allow differentiation between them. This

technique has recently been used to differentiate between magmatic and mantle CO2 and

CH4 reservoirs at St Ives (Kendrick et al., 2006). Noble gas and halogen analyses of

aqueous and aqueous-carbonic fluid inclusions from New Celebration are in progress at

the University of Melbourne and the results may provide better constraints on the


191

source(s) of mineralizing and non-mineralizing fluids. Stable isotopic analysis of carbon

in methane and aqueous-carbonic fluid inclusions may also provide better constraints on

the origin of hydrothermal fluids. This technique was tried at New Celebration but was

unsuccessful due to the small fluid inclusion size and low concentrations of CO2 and

CH4.

Geochronological constraints on the timing of gold mineralization were outside

the scope of this study and therefore the ages of granite stock emplacement and gold

mineralization are yet undetermined. Fluid inclusion evidence from this study indicates

that Stage II mineralization took place at lower temperatures and shallower crustal

levels than Stage I, suggesting that the two events were separated by a period of uplift

and erosion, of unknown duration. Maximum ages of gold mineralization could be

resolved by U-Pb SHRIMP (sensitive-high resolution ion microprobe) dating of zircons

within the host M1 (Stage I) and M2 (Stage II) porphyry dikes. Absolute mineralization

ages could be constrained by Pb/Pb dating of mineralization-related hydrothermal

monazite (cf. Nguyen, 1997, Revenge deposit, St Ives), by Re/Os dating of ore-stage

pyrite, or by Ar/Ar dating of sericite inclusions in ore-stage pyrite (Phillips and Miller,

2006).

REFERENCES

192

REFERENCES

Afifi, A. M., Kelly, W. C., and Essene, E. J., 1988, Phase relations among tellurides, sulfides, and oxides; Pt. II, Applications to telluride-bearing ore deposits: Economic Geology, v. 83, p. 395-404.

Ahmad, M., Solomon, M., and Walshe, J. L., 1987a, The formation of the quartz-gold-telluride veins of the Emporor mine, Fiji, in Brennan, E., ed., Pacific Rim Congress '87, An International Congress on the Geology, Structure, Mineralization and Economics of the Pacific Rim, Australasian Institute of Mining and Metallogeny, p. 1-14.

Ahmad, M., Solomon, M., and Walshe, J. L., 1987b, Mineralogical and geochemical studies of the Emperor gold telluride deposit, Fiji: Economic Geology, v. 83, p. 345-370.

Allan, M. M., Yardley, B. W. D., Forbes, L. J., Shmulovich, K. I., Banks, D. A., and Shepherd, T. J., 2005, Validation of LA-ICP-MS fluid inclusion analysis with synthetic fluid inclusions: American Mineralogist, v. 90, p. 1767-1775.

Amaro, D., 1985, Pyrite morphology, grainsize distribution and trace element content as indicators of gold mineralisation processes: Unpub. BSc (Hons) thesis, University of Western Australia.

Archibald, N. J., 1985, The stratigraphy and tectono-metamorphic history of the Kambalda-Tramways area, Western Australia, Western Mining Corporation Unpublished Report, p. 66.

Archibald, N. J., 1992, Jubilee gold deposit; geology, structure and mineralisation: Unpublished company report, p. 10.

Archibald, N. J., Bettenay, L. F., Binns, R. A., Groves, D. I., and Gunthorpe, R. J., 1978, The evolution of Archaean greenstone terrains, Eastern Goldfields Province, Western Australia: Precambrian Research, v. 6, p. 103-131.

Audetat, A., Gunther, D., and Heinrich, C. A., 1998, Formation of a Magmatic-Hydrothermal Ore Deposit: Insights with LA-ICP-MS Analysis of Fluid Inclusions: Science, v. 279, p. 2091-2094.

Audetat, A., Gunther, D., and Heinrich, C. A., 2000, Causes for Large-Scale Metal Zonation around Mineralized Plutons: Fluid Inclusion LA-ICP-MS Evidence from the Mole Granite, Australia: Economic Geology, v. 95, p. 1563-1581.

Audetat, A., Pettke, T., Heinrich, C. A., and Bodnar, R. J., 2008, Special Paper: The Composition of Magmatic-Hydrothermal Fluids in Barren and Mineralized Intrusions: Economic Geology, v. 103, p. 877-908.

Baggott, M. S., Vielreicher, N., Groves, D. I., McNaughton, N. J., and Gebre-Mariam, M., in press, Evidence for post ca 2.66 Ga Archean lode-gold mineralization in the Yandal belt, Western Australia, from the high-level, brittle-style Jundee-Nimary gold deposits: Economic Geology.

Bailly, L., Bouchot, V., Beny, C., and Milesi, J.-P., 2000, Fluid inclusion study of stibnite using infrared microscopy: an example from the Brouzils antimony deposit (Vendee, Armorican Massif, France): Economic Geology, v. 95, p. 221-226.

Barley, M. E., and Groves, D. I., 1987, Hydrothermal alteration of Archaean supracrustal sequences in the central Norseman-Wiluna belt, in Ho, S. E., and Groves, D. I., eds., Recent advances in understanding Precambrian gold deposits, University of Western Australia, Geology Department and University Extension, Publication No. 11, p. 51-66.

REFERENCES

193

Bartch, R. D., 1990, Lady Bountiful gold deposit, in Hughes, F. E., ed., Geology of the Mineral Deposits of Australia and Papua New Guinea, Australian Institute of Mining and Metallurgy Monograph 14, p. 401-404.

Bartram, G. D., and McCall, G. J. H., 1971, Wall-rock alteration associated with auriferous lodes in the Golden Mile, Kalgoorlie: Geological Society of Australia Special Publications, v. 3, p. 191-199.

Bateman, R. J., and Hagemann, S. G., 2004, Gold mineralisation throughout about 45 Ma of Archaean orogenesis: protracted flux of gold in the Golden Mile, Yilgarn Craton, Western Australia: Mineralium Deposita, v. 39, p. 536-559.

Bateman, R. J., Hagemann, S. G., McCuaig, T. C., and Swager, C., 2001, Protracted gold mineralisation throughout Archaean orogenesis in the Kalgoorlie camp, Yilgarn Craton, Western Australia: structural, mineralogical and geochemical evolution, in Hagemann, S. G., Neumayr, P., and Witt, W. K., eds., World-class Gold Camps and Deposits in the Eastern Yilgarn Craton, Western Australia, with Special Emphasis on the Eastern Goldfields Province, Record 2001/17, Western Australian Geological Survey, p. 63-98.

Benning, L. G., and Seward, T. M., 1996, Hydrosulphide complexing of gold(I) in hydrothermal solutions from 150 to 500°C and 500 to 1500 bars: Geochimica et Cosmochimica Acta, v. 60, p. 1849-1871.

Bierlein, F., and Crowe, D., 2000, Phanerozoic orogenic lode gold deposits, in Hagemann, S. G., and Brown, P. E., eds., Gold in 2000, Reviews in Economic Geology, v. 13, p. 103-139.

Blewett, R. S., Cassidy, K. F., Champion, D. C., Henson, P. A., Goleby, B. S., Jones, L., and Groenewald, P. B., 2004, The Wangkathaa Orogeny: an example of episodic regional `D2' in the late Archaean Eastern Goldfields Province, Western Australia: Precambrian Research, v. 130, p. 139 - 159.

Blewett, R. S., and Hitchman, A. P., 2006, 3D Geological models of the eastern Yilgarn Craton Project Y2, Geoscience Australia Record 2006/05, p. 276.

Bodnar, R. J., and Vityk, M. O., 1994, Interpretation of microthermometric data for H2O-NaCl inclusions, in De Vivo, B., and Frezzotti, M. L., eds., Fluid Inclusions in Minerals: Methods and Applications, Virginia Polytechnic Institute Press, p. 117-130.

Borisenko, A. S., 1977, Study of the salt composition of solutions in gas-liquid inclusions in minerals by the cryometric method: Soviet Geology and Geophysics, v. 18, p. 11-19.

Boullier, A., Firdaous, K., and Robert, F., 1998, On the significance of aqueous fluid inclusions in gold-bearing quartz vein deposits from the Southeastern Abitibi subprovince (Quebec, Canada): Economic Geology, v. 93, p. 216-223.

Boulter, C. A., Fotios, M. G., and Phillips, G. N., 1987, The Golden Mile, Kalgoorlie: A giant gold deposit localized in ductile shear zones by structurally induced infiltration of an auriferous metamorphic fluid: Economic Geology, v. 82, p. 1661-1678.

Bowers, T. S., 1991, The deposition of gold and other metals: Pressure-induced fluid immiscibility and associated stable isotope signatures: Geochimica et Cosmochimica Acta, v. 55, p. 2417.

Bray, C. J., Spooner, E. T. C., and Thomas, A. V., 1991, Fluid inclusion volatile analysis by heated crushing, on-line gas chromatography: application to Archaean fluids: Journal of Geochemical Exploration, v. 42, p. 167-192

Brown, P. E., and Hagemann, S. E., 1995, MacFlinCor and its application to fluids in

Archean lode-gold deposits: Geochimica et Cosmochimica Acta, v. 59, p. 3943-3952.

REFERENCES

194

Bucci, L. A., Hagemann, S. G., Groves, D. I., and Standing, J. G., 2002, The Archean Chalice gold deposit: a record of complex, multistage, high-temperature hydrothermal activity and gold mineralisation associated with granitic rocks in the Yilgarn Craton, Western Australia: Ore Geology Reviews, v. 19, p. 23.

Bucci, L. A., McNaughton, N. J., Fletcher, I. R., Groves, D. I., Kositcin, N., Stein, H. J., and Hagemann, S. G., 2004, Timing and Duration of High-Temperature Gold Mineralization and Spatially Associated Granitoid Magmatism at Chalice, Yilgarn Craton, Western Australia: Economic Geology, v. 99, p. 1123-1144.

Buchholz, P., Oberthur, T., Luders, V., and Wilkinson, J., 2007, Multistage Au-As-Sb Mineralization and Crustal-Scale Fluid Evolution in the Kwekwe District, Midlands Greenstone Belt, Zimbabwe: A Combined Geochemical, Mineralogical, Stable Isotope, and Fluid Inclusion Study: Economic Geology, v. 102, p. 347-378.

Burnham, C. W., 1979, Magmas and hydrothermal fluids, in Barnes, H. L., ed., Geochemistry of hydrothermal ore deposits: New York, Wiley Interscience, p. 71-136.

Burrows, D. R., and Spooner, E. T. C., 1986, The McIntyre Cu-Au deposit, Timmins, Ontario, Canada, in Macdonald, A. J., ed., Proceedings of Gold '86, an international symposium on the Geology of Gold Deposits: Toronto, p. 23-39.

Burrows, D. R., and Spooner, E. T. C., 1987, Generation of a magmatic H2O-CO2 fluid enriched in Mo, Au, and W within an Archean sodic granodiorite stock, Mink Lake, northwestern Ontario: Economic Geology, v. 82, p. 1931-1957.

Burrows, D. R., Wood, P. C., and Spooner, E. T. C., 1986, Carbon isotope evidence for a magmatic origin for Archaean gold-quartz vein deposits: Nature, v. 321, p. 851-854.

Callaghan, T., 2001, Geology and Host-Rock Alteration of the Henty and Mount Julia Gold Deposits, Western Tasmania: Economic Geology, v. 96, p. 1073-1088.

Cameron, E. M., 1988, Archean gold: relation to granulite formation and redox zoning in the crust: Geology, v. 16, p. 109-112.

Cameron, E. M., 1993, Precambrian Gold: perspectives from the top and bottom of shear-zones: Canadian Mineralogist, v. 31, p. 917-944.

Cameron, E. M., and Hattori, K., 1987, Archean gold mineralization and oxidized hydrothermal fluids: Economic Geology, v. 82, p. 1177-1191.

Cameron, G., 1998, The hydrothermal evolution and genesis of the Porgera gold deposit, Papua New Guinea: Unpub. PhD thesis, Australian National University, 137 p.

Cameron, G., Wall, V. J., Walshe, J. L., and Heinrich, C. A., 1995, Gold mineralization at the the Porgera deposit, Papua New Guinea, in response to fluid mixing: PACRIM '95 Conference, Auckland, New Zealand, 1995, p. 99-100.

Carew, M. J., Mark, G., Oliver, N. H. S., and Pearson, N., 2006, Trace element geochemistry of magnetite and pyrite in Fe oxide (±Cu–Au) mineralised systems: Insights into the geochemistry of ore-forming fluids: Geochimica et Cosmochimica Acta, v. 70, p. A83.

Cassidy, K., and Bennett, J., 1993, Gold mineralisation at the Lady Bountiful Mine, Western Australia: An example of a granitoid-hosted Archaean lode gold deposit: Mineralium Deposita, v. 28, p. 388.

Champion, D. C., and Sheraton, J. W., 1997, Geochemistry and Nd isotope systematics of Archaean granites of the Eastern Goldfields, Yilgarn Craton, Australia: implications for crustal growth processes: Precambrian Research, v. 83, p. 109.

Channer, D. M. D., and Spooner, E. T. C., 1991, Grant 364. Multiple fluid inclusion generations in variably deformed quartz: Hollinger-McIntyre and Ker Addison-

REFERENCES

195

Chesterville Archean gold-bearing quartz-vein systems, Northern Ontario: Ontario Geological Survey Miscellaneous Paper 156, p. 47-64.

Clark, M. E., 1980, Localization of gold, Mt Charlotte, Kalgoorlie, Western Australia: Unpub. BSc (Honours) thesis, University of Western Australia, 128 p.

Clark, M. E., 1987, The geology of the Victory gold mine, Kambalda, Western Australia: Unpub. PhD thesis, Queen's University

199 p. Clark, M. E., Archibald, N. J., and Hodgson, C. J., 1986, The structural and

metamorphic setting of the Victory gold mine, Kambalda, Western Australia, in Macdonald, A. J., ed., Gold '86: Willowdale, Ontario, Konsult International Incorporated, p. 243-254.

Clark, M. E., Carmichael, D. M., Hodgson, C. J., and Fu, M., 1989, Wall-rock alteration, Victory gold mine, Kambalda, Western Australia: Processes and P-T-X(CO2) conditions of metasomatism: Economic Geology Monograph, v. 6, p. 445-459.

Cline, J. S., and Bodnar, R. J., 1991, Can economic porphyry copper mineralization be generated by a typical calc-alkaline melt?: Journal of Geophysical Research, v. 96, p. 8113-8126.

Clout, J. M. F., 1989, Structural and isotopic studies of the Golden Mile gold-telluride deposit, Kalgoorlie, W.A.: Unpub. PhD thesis, Monash University, Melbourne, Australia.

Clout, J. M. F., Cleghorn, J. H., and Eaton, P. C., 1990, Geology of the Kalgoorlie Gold Field, in Hughes, F. E., ed., Geology of the Mineral Deposits of Australia and Papua New Guinea: Melbourne, Australasian Institute of Mining and Metallurgy, p. 411-431.

Collins, P. L. F., 1979, Gas hydrates in CO2-bearing fluid inclusions and the use of freezing for estimation of salinity: Economic Geology, v. 74, p. 1435-1444.

Colvine, A. C., 1989, An empirical model for the formation of Archean gold deposits: Products of final cratonization of the Superior Province, Canada, in Keays, R. R., Ramsay, W. R. H., and Groves, D. I., eds., The geology of gold deposits; the perspective in 1988, Economic Geology Monograph Volume 6, p. 37-53.

Colvine, A. C., Fyon, J. A., Heather, K. B., Marmont, S., Smith, P. M., and Troop, D. G., 1988, Archean Lode Gold Deposits in Ontario, Ontario Geological Survey Miscellaneous Paper 139, p. 136.

Cooke, D. R., and McPhail, D. C., 2001, Epithermal Au-Ag-Te Mineralization, Acupan, Baguio District, Philippines: Numerical Simulations of Mineral Deposition: Economic Geology, v. 96, p. 109-131.

Cooke, D. R., and Simmons, S. F., 2000, Characteristics and genesis of epithermal gold deposits: SEG Reviews, v. 13, p. 221-244.

Copeland, I. K., 1998, Jubilee gold deposit, Kambalda: Australasian Institute of Mining and Metallurgy Monograph 22, p. 219-224.

Couture, J. F., and Pilote, P., 1993, The geology and alteration patterns of a disseminated, shear zone-hosted mesothermal gold deposit: the Francoeur 3 Deposit, Rouyn-Noranda, Quebec

Economic Geology, v. 88, p. 1664-1684. Cox, S. F., Knackstedt, M. A., and Braun, J., 2001, Principles of Structural Control on

Permeability and Fluid Flow in Hydrothermal Systems, in Richards, J. P., and Tosdal, R. M., eds., Structural Controls on Ore Genesis, SEG Reviews, v. 14, p. 1-24.

Cox, S. F., and Ruming, K., 2004, The St Ives mesothermal gold system, Western Australia - a case of golden aftershocks?: Journal of Structural Geology, v. 26, p. 1109-1125.

REFERENCES

196

Cox, S. F., Sun, S. S., Etheridge, M. A., Wall, V. J., and Potter, T. F., 1995, Structural and geochemical controls on the development of turbidite-hosted gold quartz vein deposits, Wattle Gully Mine, Central Victoria, Australia: Economic Geology, v. 90, p. 1722-1746.

Crawford, M. L., 1981, Phase equilibria in aqueous fluid inclusions, in Hollister, L. S., and Crawford, M. L., eds., Short Course in Fluid Inclusions: Applications to Petrology, 6, Mineralogical Association of Canada, p. 75-100.

de-Ronde, C. E. J., Spooner, E. T. C., de-Wit, M. J., and Bray, C. J., 1992, Shear Zone-related, Au Quartz Vein Deposits in the Barberton Greenstone Belt, South Africa: Field and Petrographic Characteristics, Fluid Properties, and Light Stable Isotope Geochemistry: Economic Geology, v. 87, p. 366-402.

Diamond, L. W., 1990, Fluid inclusion evidence for P-V-T-X evolution of hydrothermal solutions in late alpine gold-quartz veins at Brusson, Val d'ayas, Northwest Italian Alps: American Journal of Science, v. 290, p. 912-958.

Diamond, L. W., 1992, Stability of clathrate hydrate + CO2 liquid + CO2 vapour + aqueous KCl-NaCl solutions: Experimental determination and application to salinity estimates of fluid inclusions: Geochimica et Cosmochimica Acta, v. 56.

Diamond, L. W., 2001, Review of the systematics of CO2-H2O fluid inclusions: Lithos, v. 55, p. 69-99.

Dielemans, P., 2000, Structural controls on gold mineralisation in the Southern Ore Zone of the Hampton-Boulder deposit, New Celebration gold mine, Western Australia: Unpub. MSc. thesis, University of Western Australia, 185 p.

Donnelly, T. H., Lambert, I. B., Oehler, D. Z., Hallberg, J. A., Hudson, D. R., Smith, J. W., Bavinton, O. A., and Golding, L. Y., 1978, A reconnaissance study of stable isotope ratios in Archean rocks from the Yilgarn block, Western Australia: Journal of the Geological Society of Australia, v. 24.

Drummond, S. E., and Ohmoto, H., 1985, Chemical evolution and mineral deposition in boiling hydrothermal systems: Economic Geology, v. 80, p. 126-147.

Duan, Z., 1992, An equation of state for the CH4-CO2-H2O system: II. Mixtures from 50-1000°C and 0-1000 bar: Geochimica et Cosmochimica Acta, v. 56, p. 2619-2631.

Eastoe, C. J., 1978, A fluid inclusion study on the Panguna porphyry copper deposit, Bougainville, Papua New Guinea: Economic Geology, v. 73, p. 721-748.

Eggler, D. H., and Kadik, A. A., 1979, The system NaAlSiO3O8-H2O-CO2 to 20 kbar pressure: I. Compositional and thermodynamic relations of liquids and vapors coexisting with albite: American Mineralogist, v. 64, p. 1036-1048.

Eilu, P., and Groves, D. I., 2001, Primary geochemical dispersion haloes around Archaean orogenic gold deposits in the Yilgarn Craton. , in Cassidy, K. F., Dunphy, J. M., and van Kranendonk, M. J., eds., Fourth international Archaean symposium; extended abstracts, Australian Geological Survey Organisation, Report # 2001/37, p. 385-387.

Eisenlohr, B. N., Groves, D. I., and Partington, G. A., 1989, Crustal scale shear zones and their significance to Archaean gold mineralisation in Western Australia: Mineralium Deposita, v. 24, p. 1-8.

Ellis, A. J., and Golding, R. M., 1963, The solubility of carbon dioxide above 100°C in water and in sodium chloride solutions: American Journal of Science, v. 261, p. 47-60.

Evans, K. A., Phillips, G. N., and Powell, R., 2006, Rock-Buffering of Auriferous Fluids in Altered Rocks Associated with the Golden Mile-Style Mineralization, Kalgoorlie Gold Field, Western Australia: Economic Geology, v. 101, p. 805-817.

REFERENCES

197

Gauthier, L., Hagemann, S. G., Cassidy, K. F., Champion, D. C., and Robert, F., in revision, Inter-mineral hornblende-plagioclase-phyric andesite dyke suite associated with Fimiston-style mineralisation at the Golden Mile, Yilgarn craton, Western Australia

Gauthier, L., Hagemann, S. G., Robert, F., and Pickens, G., 2004, New constraints on the architecture and timing of the giant Golden Mile gold deposit, Kalgoorlie, Western Australia, in Muhling, J. R., Goldfarb, R. J., Vielreicher, N., Bierlein, F., Stumpfl, E., Groves, D. I., and Kenworthy, S., eds., SEG 2004: Predictive Mineral Discovery Under Cover; Extended Abstracts, Centre for Global Metallogeny, The University of Western Australia, Publication No. 33, p. 353-356.

Gebre-Mariam, M., Groves, D. I., and McNaughton, N. J., 1997, Aqueous and CO2- and CH4- rich inclusions at the Archean Golden Kilometre gold deposit: Multiple fluid sources and depositional mechanisms: Chronique de la Recherce Miniere, v. 529, p. 59-73.

Gebre-Mariam, M., Groves, D. I., McNaughton, N. J., and Vearncombe, J. A., 1993, Archaean Au−Ag mineralisation at Racetrack, near Kalgoorlie, Western Australia: a high crustal-level expression of the Archaean composite lode-gold system Mineralium Deposita, v. 28, p. 375-387.

Gebre-Mariam, M., Hagemann, S. G., and Groves, D. I., 1995, A classification scheme for epigenetic Archean lode-gold deposits: Mineralium Deposita, v. 30, p. 408-410.

Gee, R. D., Baxter, J. L., and Wilde, S. A., 1981, Crustal development in the Archaean Yilgarn Block, Western Australia: Geological Society of Australia Special Publication, v. 7, p. 43-56.

Gehrig, M., Lentz, H., and Franck, E. U., 1980, Phase equilibria and pVT of binary and ternary mixtures of water, carbon dioxide and sodium chloride up to 3 kb and 550 degrees C: Mineralogical Society Bulletin, v. 49, p. 6.

Gemuts, I., and Theron, A., 1975, The Archean between Coolgardie and Norseman-stratigraphy and mineralization, in Knight, C. L., ed., Economic Geology of Australia and Papua New Guinea, Volume 1, Metals Parkville, Australia,, The Australasian Institute of Mining and Metallurgy, Monograph 5, p. 66-74

Goldfarb, R. J., Ayuso, R., Miller, M. L., Ebert, S. W., Marsh, E. E., Petsel, S. A.,

Miller, L. D., Bradley, D., Johnson, C., and McClelland, W., 2004, The Late Cretaceous Donlin Creek Gold Deposit, Southwestern Alaska: Controls on Epizonal Ore Formation: Economic Geology, v. 99, p. 643-671.

Goldfarb, R. J., Baker, T., Dube, B., Groves, D. I., Hart, C. J. R., and Gosselin, P., 2005, Distribution, character, and genesis of gold deposits in metamorphic terranes, in Hedenquist, J. W., Thompson, J. F. H., Goldfarb, R. J., and Richards, J. P., eds., Economic Geology 100th Anniversary Volume, Society of Economic Geologists, p. 407-450.

Goldfarb, R. J., Groves, D. I., and Gardoll, S., 2001, Orogenic gold and geologic time: a global synthesis: Ore Geology Reviews, v. 18, p. 1.

Goldfarb, R. J., Newberry, R. J., Pickthorn, W. J., and Gent, C. A., 1991, Oxygen, hydrogen, and sulphur isotope studies in the Juneau gold belt, southeastern Alaska: constraints on the origin of hydrothermal fluids: Economic Geology, v. 86, p. 66-80.

Goldfarb, R. J., Snee, L. W., and Pickthorn, W. J., 1993, Orogenesis, high-T thermal events, and gold vein formation within metamorphic rocks of the Alaskan cordillera: Mineralogical Magazine, v. 57, p. 375-394.

REFERENCES

198

Golding, S. D., 1982, An isotopic and geochemical study of gold mineralization in the Kalgoorlie-Norseman region, Western Australia: Unpub. PhD thesis, University of Queensland.

Golding, S. D., 1984, Stable isotope and geochemical studies of porphyry-related gold mineralization, Kambalda, Western Mining Corporation, Unpublished Report.

Golding, S. D., Barley, M. E., Cassidy, K., Groves, D. I., Ho, S. E., Hronsky, J. M. A., McNaughton, N. J., Sang, J. H., and Turner, J. V., 1990a, Oxygen and hydrogen isotope studies, in Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold deposits of the Archaean Yilgarn block, Western Australia: Nature, genesis and exploration guides, Geology Department (Key Centre) and University Extension, the University of Western Australia, Publication No. 20, p. 252-258.

Golding, S. D., Clark, M. E., Keele, R. A., Wilson, A. F., and Keays, R. R., 1990b, Geochemistry of Archaean epigenetic gold deposits in the Eastern Goldfields Province, Western Australia, in Herbert, H. K., and Ho, S. E., eds., Stable Isotopes and Fluid Processes in Mineralization, Geology Department and University Extension, the University of Western Australia, Publication No. 23, p. 141-176.

Golding, S. D., Groves, D. I., McNaughton, N. J., Barley, M. E., and Rock, N. M., 1987, Carbon isotopic composition of carbonates from contrasting alteration styles in supracrustal rocks of the Norseman-Wiluna belt, Yilgarn Block, Western Australia: Their significance to the source of archaean auriferous fluids, in Ho, S. E., and Groves, D. I., eds., Recent Advances in Understanding Precambrian Gold Deposits, The Geology Department and University Extension, The University of Western Australia, Publication No. 11, p. 215-238.

Golding, S. D., Groves, D. I., McNaughton, N. J., Mikucki, E., and Sang, J. H., 1990c, Sulfur isotope studies, in Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold deposits of the Yilgarn Block, Western Australia: Nature, genesis and exploration guides, University of Western Australia, Geology Department and University Extension, v. 20p. 259-262.

Golding, S. D., and Wilson, A. F., 1987, Oxygen and hydrogen isotope relationships in Archaean gold deposits of the Eastern Goldfields Province, Western Australia: Constraints on the source of Archaean gold-bearing fluids, in Ho, S. E., and Groves, D. I., eds., Recent Advances in Understanding Precambrian Gold Deposits, The Geology Department and University Extension, The University of Western Australia, Publication No. 11, p. 203-213.

Goldstein, R. M., and Reynolds, T. J., 1994, Systematics of fluid inclusions in diagenetic minerals: SEPM Short Course 31, Society for Sedimentary Geology, 199 p.

Goleby, B. R., Blewett, R. S., Fomin, T., Fishwick, S., Reading, A. M., Henson, P. A., Kennett, B. L. N., Champion, D. C., Jones, L., Drummond, B. J., and Nicoll, M., 2006, An integrated multi-scale 3D seismic model of the Archaean Yilgarn Craton, Australia: Tectonophysics, v. 420, p. 75.

Goleby, B. R., Korsch, R. J., Fomin, T., Bell, B., Nicoll, M. G., Drummond, B. J., and Owen, A. J., 2002, Preliminary 3-D geological model of the Kalgoorlie region, Yilgarn Craton, Western Australia, based on deep seismic-reflection and potential-field data: Australian Journal of Earth Sciences, v. 49, p. 917-933.

Goleby, B. R., Korsch, R. J., Fomin, T., Owen, A. J., and Bell, B., 2000, The AGCRC's 1999 Yilgarn deep seismic survey, Australian Geological Survey Organisation, 2000/34, p. 52-64.

Goscombe, B., 2009, Metamorphic evolution and integrated terrane analysis of the eastern Yilgarn Craton; rationale, methods, outcomes and interpretation, Geoscience Australia Record 2009/23, 270 p.

REFERENCES

199

Goscombe, B., Blewett, R. S., K., C., Maas, R., and Groenewald, B. A., 2007, Broad thermo-barometric evolution of the Eastern Goldfields Superterrane, in Bierlein, F. P., and Knox-Robinson, C. M., eds., Proceedings of Geoconferences (WA) Inc. Kalgoorlie '07 Conference, Kalgoorlie '07; old ground, new knowledge, Geoscience Australia Record 2007/14, p. 33-38.

Graney, J. R., and Kesler, S. E., 1995, Gas composition of fluid in ore deposits: is there a relation to magmas?, in H, T. J. F., ed., Magmas, Fluids and Ore Deposits, Mineralogical Association of Canada Short Course Series 23., p. 221–245.

Gresham, J. J., 1991, Kambalda: history of a mining town: Melbourne, Western Mining Corporation Limited, 114 p.

Gresham, J. J., and Loftus-Hills, G. D., 1981, The geology of the Kambalda Nickel Field, Western Australia: Economic Geology, v. 76, p. 1373-1416.

Griffin, T. J., 1990, Geology of the granite-greenstone terrane of the Lake Lefroy and Cowan 1:100 000 sheets, Western Australia, Geological Survey of Western Australia, Report 32, p. 44.

Groves, D. I., 1990, Excursion no. 3: Eastern Goldfields mineral deposits. 1: Overview of gold mineralization in the Norseman-Wiluna belt, in Ho, S. E., Glover, J. E., and Muhling, J. R., eds., Third international Archaean symposium excursion guidebook, Geology Department and University Extension, University of Western Australia , Publication no. 21, p. 307-317.

Groves, D. I., 1993, The crustal continuum model for late-Archean lode-gold deposits of the Yilgarn Block, Western Australia: Mineralium Deposita, v. 28, p. 366-374.

Groves, D. I., Barley, M. E., Barnicoat, A. C., Cassidy, K., Fare, R. J., Hagemann, S. G., Ho, S. E., Hronsky, J. M. A., Mikucki, E., Mueller, A. G., McNaughton, N. J., Perring, C. S., Ridley, J. R., and Vearncombe, J. A., 1992, Sub-greenschist to granulite-hosted Archaean lode-gold deposits of the Yilgarn Craton: a depositional continuum from deep-sourced hydrothermal fluids in crustal-scale plumbing systems, in Glover, J. E., and Ho, S. E., eds., The Archean: Terrains, Processes and Metallogeny: Perth, Geology Department (Key Centre) and University Extension, University of Western Australia, Publication No. 22, p. 325-337.

Groves, D. I., Barley, M. E., and Ho, S. E., 1989, Nature, genesis and tectonic setting of mesothermal gold mineralisation in the Yilgarn Block, Western Australia, in Keays, R. R., Ramsay, W. R. H., and Groves, D. I., eds., The Geology of Gold Deposits: The Perspective in 1988. Economic Geology Monograph 6, p. 71-85.

Groves, D. I., and Foster, R. P., 1993, Archaean lode gold deposits, in Foster, R. P., ed., Gold Metallogeny and Exploration: Glasgow, Blackie and Son, p. 63-103

Groves, D. I., Goldfarb, R. J., Gebre-Mariam, M., Hagemann, S. G., and Robert, F.,

1998, Orogenic gold deposits: A proposed classification in the context of their crustal distribution and relationship to other gold deposit types: Ore Geology Reviews, v. 13, p. 7.

Groves, D. I., Goldfarb, R. J., Knox-Robinson, C. M., Ojala, J., Gardoll, S., Yun, G. Y., and Holyland, P., 2000, Late-kinematic timing of orogenic gold deposits and significance for computer-based exploration techniques with emphasis on the Yilgarn Block, Western Australia: Ore Geology Reviews, v. 17, p. 1.

Groves, D. I., Goldfarb, R. J., Robert, F., and Hart, C. J. R., 2003, Gold Deposits in Metamorphic Belts: Overview of Current Understanding, Outstanding Problems, Future Research, and Exploration Significance: Economic Geology, v. 98, p. 1-29.

REFERENCES

200

Groves, D. I., and Phillips, G. N., 1987, The genesis and tectonic controls on Archaean gold deposits of the Western Australian shield: A metamorphic-replacement model: Ore Geology Reviews, v. 2, p. 287-322.

Guha, J., and Kanwar, R., 1987, Vug brines - fluid inclusions: A key to understanding of secondary gold enrichment processes and the evolution of deep brines in the Canadian Shield, in Fritz, P., and Frape, S. K., eds., Saline water and gases in the crystalline rocks, Geological Association of Canada Special Paper v. 33, p. 95-101.

Guillemette, N., and Williams-Jones, A. E., 1993, Genesis of the Sb-W-Au deposits at Ixtahuacan, Guatemala: evidence from fluid inclusions and stable isotopes Mineralium Deposita, v. 28, p. 167-180.

Gunther, D., Audetat, A., Frischknecht, R., and Heinrich, C. A., 1998, Quantitative analysis of major, minor and trace elements in fluid inclusions using laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS): Journal of Analytical Atomic Spectroscopy, v. 13, p. 263-270.

Gunther, D., Frischknecht, R., Heinrich, C. A., and Kahlert, H.-J., 1997, Capabilities of an argon fluoride 193 nm Excimer laser for laser ablation inductively coupled plasma mass spectrometry microanalysis of geological materials: Journal of Analytical Atomic Spectroscopy, v. 12, p. 939-944.

Hagemann, S. E., and Cassidy, K., 2000, Archean orogenic lode gold deposits, in Hagemann, S. E., and Brown, P. E., eds., Gold in 2000, SEG Reviews v. 13, p. 9-68.

Hagemann, S. G., Bateman, R. J., Crowe, D., and Vielreicher, R. M., 1999, In situ sulfur isotope composition of pyrites from the Fimiston- and Oroya-style gold lodes in the Golden Mile Camp, Kalgoorlie; implications for sulfur source(s) and depositional processes: Geological Society of America Annual Conference Abstracts, v. 31, p. A-245.

Hagemann, S. G., and Cassidy, D. F., 2001, World-class gold camps and deposits in the Eastern Goldfields Province, Yilgarn Craton: diversity in host rocks, structural controls and mineralization styles, in Hagemann, S. G., Neumayr, P., and Witt, W. K., eds., World-class Gold Camps and Deposits in the Eastern Yilgarn Craton, Western Australia, with Special Emphasis on the Eastern Goldfields Province, p. 7-44.

Hagemann, S. G., Gebre-Mariam, M., and Groves, D. I., 1994, Surface-water influx in shallow-level Archaean lode gold deposits in Western Australia: Geology, v. 22, p. 1067-1070.

Hagemann, S. G., Groves, D. I., Ridley, J. R., and Vearncombe, J. A., 1993, The Archean lode gold deposits at Wiluna, Western Australia: High-level brittle-style mineralization in a strike-slip regime: Economic Geology, v. 87, p. 1022-1053.

Hagemann, S. G., and Lüders, V., 2003, P-T-X conditions of hydrothermal fluids and precipitation mechanism of stibnite-gold mineralization at the Wiluna lode-gold deposits, Western Australia: Conventional and infrared microthermometric constraints: Mineralium Deposita, v. 38, p. 936-952.

Hall, D. L., and Bodnar, R. J., 1990, Methane in fluid inclusions from granulites: A product from hydrogen diffusion?: Geochimica et Cosmochimica Acta, v. 54, p. 641-651.

Harbi, H., 1997, Origin of the stockwork mineralization at Kalgoorlie, Western Australia: Unpub. PhD thesis, University of Western Australia.

Haynes, F. M., 1988, Fluid inclusion evidence of basinal brines in Archean basement, Thunder Bay Pb-Zn-Ba district, Ontario, Canada: Canadian Journal of Earth Sciences, v. 25, p. 1884-1894.

REFERENCES

201

Haynes, F. M., and Kesler, S. E., 1987, Chemical evolution of brines during Mississippi Valley-type mineralization: Evidence from East Tennessee and Pine Point: Economic Geology, v. 82, p. 53-71.

Haynes, F. M., and Kesler, S. E., 1988, Compositions and sources of mineralizing fluids for chimney and manto limestone-replacement ores in Mexico: Economic Geology, v. 83, p. 1985-1992.

Hedenquist, J. W., and Henley, R. W., 1985, The importance of CO2 on freezing point measurements of fluid inclusions: evidence from active geothermal systems and implications for epithermal ore deposition: Economic Geology, v. 80, p. 1379-1406.

Heinrich, C. A., Henley, R. W., and Seward, T. M., 1989, Hydrothermal Systems: Adelaide, Australian Mineral Foundation, 74 p.

Ho, S. E., 1986, A fluid inclusion study of Archaean gold deposits of the Yilgarn Block, Western Australia: Unpub. PhD thesis, University of Western Australia, 90 p.

Ho, S. E., 1987, Fluid inclusions: Their potential as an exploration tool for Archaean gold deposits, in Ho, S. E., and Groves, D. I., eds., Recent advances in understanding Precambrian gold deposits, Publication no. 11, Geology Department and University Extension, University of Western Australia, p. 239-263.

Ho, S. E., Bennett, J., Cassidy, K., Hronsky, J. M. A., Mikucki, E., and Sang, J. H., 1990, Nature of ore fluid, and transportational and depositional conditions in sub-amphibolite facies deposits, in Ho, S. E., Groves, D. I., and Bennett, J., eds., University of Western Australia, Geology Department (Key Centre) and University Extension, Publication 20, p. 198-211.

Ho, S. E., Groves, D. I., McNaughton, N. J., and Mikucki, E. J., 1992, The source of ore fluids and solutes in Archaean lode-gold deposits of Western Australia: Journal of Volcanology and Geothermal Research, v. 50, p. 173-196.

Ho, S. E., McNaughton, N. J., and Groves, D. I., 1994, Criteria for determining initial lead isotopic compositions of pyrite in Archean lode-gold deposits: a case study at Victory, Kambalda, Western Australia: Chemical Geology, v. 111, p. 57-84.

Ho, S. E., McQueen, K. G., McNaughton, N. J., and Groves, D. I., 1995, Lead isotope systematics and pyrite trace element geochemistry of two granitoid-associated mesothermal gold deposits in the southeastern Lachlan fold belt: Economic Geology, v. 90, p. 1818-1830.

Hodge, J. L., 1997, Geochemistry of magnetite from volcanic rocks of the North Island, New Zealand: Unpub. MSc thesis, University of Auckland, 138 p.

Hodge, J. L., Hagemann, S. G., Neumayr, P., Davidson, G., and Banks, D., in revision, The New Celebration Gold Deposit: P-T-X-t Fluid Evolution and Two Stages of Gold Mineralization within the Crustal-scale Boulder-Lefroy Fault Zone, Yilgarn Craton, Western Australia.

Hodgson, C. J., 1993, Mesothermal lode-gold deposits, in Kirkham, R. V., Sinclair, W. D., Thorpe, R. I., and Duke, J. M., eds., Mineral Deposit Modeling, Special Paper 40, Geological Association of Canada, p. 635-678.

Hodgson, C. J., and Troop, D. G., 1988, A new computer aided methodology for area selection in gold exploration: A case study from the Abitibi greenstone belt: Economic Geology, v. 83, p. 952-977.

Hodkiewicz, P., 2003, The Interplay Between Physical and Chemical Processes in the Formation of World-Class Orogenic Gold Deposits in the Eastern Goldfields Province, Western Australia: Unpub. PhD thesis, University of Western Australia, 198 p.

Hodkiewicz, P., Groves, D. I., Davidson, G., Weinberg, R. F., and Hagemann, S. G., 2009, Influence of structural setting on sulphur isotopes in Archean orogenic

REFERENCES

202

gold deposits, Eastern Goldfields Province, Yilgarn, Western Australia: Mineralium Deposita, v. 44, p. 129-150.

Hoernes, S., and van Reenen, D. D., 1992, The oxygen isotopic composition of granulites and regressed granulites from theLimpopo bet as a monitor of fluid-rock interaction: Precambrian Research, v. 55, p. 353-364.

Hofstra, A. H., and Cline, J. S., 2000, Characteristics and models for Carlin-type gold deposits: SEG Reviews, v. 13, p. 163-220.

Honma, H., and Itihara, Y., 1981, Distribution of ammonium in minerals of metamorphic and granitic rocks: Geochimica et Cosmochimica Acta, v. 45, p. 983-988.

Huston, D. L., Power, M., Gemmell, J. B., and Large, R. R., 1995a, Design, calibration and geological application of the first operational Australian laser ablation sulphur isotope microprobe: Australian Journal of Earth Sciences, v. 42, p. 549-555.

Huston, D. L., Sie, S. H., Suter, G. F., Cooke, D. R., and Both, R. A., 1995b, Trace elements in sulfide minerals from eastern Australian volcanic-hosted massive sulfide deposits; Part I, Proton microprobe analyses of pyrite, chalcopyrite, and sphalerite, and Part II, Selenium levels in pyrite; comparison with delta 34 S values and implications for the source of sulfur in volcanogenic hydrothermal systems: Economic Geology, v. 90, p. 1167-1196.

Jacobs, G. K., and Kerrick, D. M., 1981, Methane: An equation of state with application to the ternary system H2O-CO2-CH4: Geochimica et Cosmochimica Acta, v. 45, p. 607-614.

Jensen, E., and Barton, M., 2000, Gold deposits related to alkaline magmatism: Reviews in Economic Geology, v. 13, p. 279-314.

Jia, Y., and Kerrich, R., 1999, Nitrogen isotope systematics of mesothermal lode gold deposits: Metamorphic, granitic, meteoric water, or mantle origin?: Geology, v. 27, p. 1051-1054.

Jia, Y., Kerrich, R., and Goldfarb, R., 2003, Metamorphic Origin of Ore-Forming Fluids for Orogenic Gold-Bearing Quartz Vein Systems in the North American Cordillera: Constraints from a Reconnaissance Study of {delta}15N, {delta}D, and {delta}18O: Economic Geology, v. 98, p. 109-123.

Jia, Y., Li, X. I. A., and Kerrich, R., 2001, Stable Isotope (O, H, S, C, and N) Systematics of Quartz Vein Systems in the Turbidite-Hosted Central and North Deborah Gold Deposits of the Bendigo Gold Field, Central Victoria, Australia: Constraints on the Origin of Ore-Forming Fluids: Economic Geology, v. 96, p. 705-721.

Kendrick, M. A., Burgess, R., Pattrick, R. A. D., and Turner, G., 2001, Fluid inclusion noble gas and halogen evidence on the origin of Cu-porphyry mineralising fluids: Geochimica et Cosmochimica Acta, v. 65, p. 2651-2668.

Kendrick, M. A., Duncan, R., and Phillips, D., 2006, Noble gas and halogen constraints on mineralizing fluids of metamorphic versus surficial origin: Mt Isa, Australia: Chemical Geology, v. 235, p. 325-351.

Kendrick, M. A., Walshe, J. L., Mark, G., Petersen, K. J., Baker, T., Phillips, D., Honda, M., Oliver, N. H. S., Fisher, L., Gillen, D., Williams, P. J., and Fu, B., 2008, Sources and reservoirs; noble gases as tools for constraining a mantle connection during orogenic-gold and IOCG mineralisation, in Korsch, R. J., and Barnicoat, A. C., eds., New perspectives; the foundations and future of Australian exploration; abstracts for the June 2008 pmd*CRC conference. Geoscience Australia Record 2008/09, p. 48-54.

Kent, A. J. R., Campbell, I. H., and McCulloch, M. T., 1995, Sm-Nd systematics of hydrothermal scheelite from the Mount Charlotte mine, Kalgoorlie, Western

REFERENCES

203

Australia: an isotopic link between gold mineralization and komatiites: Economic Geology, v. 90, p. 2329-2335.

Kent, A. J. R., and McDougall, I., 1995, 40Ar-39Ar and U-Pb age constraints on the timing of gold mineralization in the Kalgoorlie goldfields, Western Australia: Economic Geology, v. 90.

Kenworthy, S., and Hagemann, S. G., 2005, Decoupled lamprophyric magmatism and gold mineralization at the Archean Darlot lode gold deposit, Western Australia, in Mao, J., and Bierlein, F. P., eds., Mineral deposit research; meeting the global challenge: Proceedings of the Biennial SGA Society for Geology Applied to Mineral Deposits Meeting 8, v. 2, p. 987-990.

Kerrich, R., 1986, The stable isotope geochemistry of Au-Ag vein deposits in metamorphic rocks, in Kyser, T. K., ed., Short Course in Stable Isotope Geochemistry of Low Temperature Fluids, 13, Mineralogical Association of Canada, p. 287-336.

Kerrich, R., 1989, Geodynamic setting and hydraulic regimes: Shear zones and mesothrmal gold deposits, in Bursnall, J. T., ed., Mineralization and shear zones, Geological Association of Canada, Short Course Notes, 6, p. 89-128.

Kerrich, R., and Cassidy, K., 1994, Temporal relationships of lode gold mineralization to accretion, magmatism, metamorphism and deformation - Archean to present: A review: Ore Geology Reviews, v. 9, p. 263-310.

Kerrich, R., and Hodder, R. W., 1982, Archean lode gold and base metal deposits - chemical evidence for metal fractionation into independent hydrothermal reservoirs: Canadian Institute of Mining and Metallurgy Special Volume, v. 24, p. 144-160.

Kerrich, R., and King, R., 1993, Hydrothermal zircon and baddeleyite in Val d'Or Archean mesothermal gold deposits: Characteristics, compositions and fluid inclusion properties: Canadian Journal of Earth Sciences, v. 30, p. 2334-2351.

Kerrich, R., and Wyman, D., 1994, The mesothermal gold lamprophyre association: significance for an accretionary geodynamic setting, supercontinent cycles and metallogenic processes: Mineralogy and Petrology, v. 51, p. 147-172.

Kilinc, I. A., and Burnham, C. W., 1972, Partitioning of chloride between a silicate melt and coexisting aqueous phase from 2 to 8 kilobars: Economic Geology, v. 67, p. 231-235.

Kishida, A., and Kerrich, R., 1987, Hydrothermal alteration zoning and gold concentration at the Kerr-Addison Archean lode gold deposit, Kirkland Lake, Ontario: Economic geology and the bulletin of the Society of Economic Geologists, v. 82, p. 649-690.

Klemm, L. M., Pettke, T., Heinrich, C. A., and Campos, E., 2007, Hydrothermal Evolution of the El Teniente Deposit, Chile: Porphyry Cu-Mo Ore Deposition from Low-Salinity Magmatic Fluids: Economic Geology, v. 102, p. 1021-1045.

Knudsen, T.-L., and Andersen, T., 1999, Petrology and geochemistry of the Tromøy Gneiss Complex, South Norway, an alleged example of Proterozoic depleted lower continental crust: Journal of Petrology, v. 40, p. 909-933.

Kreuzer, O. P., 2005, Intrusion-Hosted Mineralization in the Charters Towers Goldfield, North Queensland: New Isotopic and Fluid Inclusion Constraints on the Timing and Origin of the Auriferous Veins: Economic Geology, v. 100, p. 1583-1603.

Lambert, I. B., Phillips, G. N., and Groves, D. I., 1984, Sulphur isotope compositions and genesis of Archaean gold mineralization, Australia and Zimbabwe, in Foster, R. P., ed., Gold '82: the Geology, Geochemistry and Genesis of Gold Deposits: Rotterdam, A.A. Balkema

p. 373-387.

REFERENCES

204

Landtwing, M. R., Heinrich, C. A., Halter, W. E., Pettke, T., Redmond, P. B., and Einaudi, M. T., 2002, Fluid evolution at the Bingham Cu-Au-Mo-Ag porphyry deposit: Geochimica et Cosmochimica Acta, v. 66, p. A430.

Langsford, N., 1989, Stratigraphy of Locations 48 and 50, Kalgoorlie Gold Workshop, p. 6.

Larcombe, C. O. G., 1912, The geology of Kalgoorlie: Australian Institute Mining Engineering, Transactions, v. 14, p. 1-327.

Large, R. R., Danyushevsky, L., Hollit, C., Maslennikov, V., Meffre, S., Gilbert, S., Bull, S., Scott, R., Emsbo, P., Thomas, H., Singh, B., and Foster, J., 2009, Gold and Trace Element Zonation in Pyrite Using a Laser Imaging Technique: Implications for the Timing of Gold in Orogenic and Carlin-Style Sediment-Hosted Deposits: Economic Geology, v. 104, p. 635-668.

Loftus-Hills, G., and Solomon, M., 1967, Cobalt, nickel and selenium as indicators of ore genesis: Mineralium Deposita, v. 2, p. 228-242.

Loucks, R. R., 2000, Precise geothermometry on fluid inclusion populations that trapped mixtures of immiscible fluids.: American Journal of Science, v. 300, p. 23-59.

Loucks, R. R., and Mavrogenes, J. A., 1999, Gold solubility in supercritical hydrothermal brines measured in synthetic fluid inclusions: Science, v. 284, p. 2159-2163.

. Lungan, A., 1986, The structural controls of the Oroya shoot: implications for the

structure of the Kalgorlie region, Western Australia: Unpub. BSc Honours thesis, University of Western Australia.

Mair, J. L., Goldfarb, R. J., Johnson, C. A., Hart, C. J. R., and Marsh, E. E., 2006, Geochemical constraints on the genesis of the Scheelite Dome intrusion-related gold deposit, Tombstone gold belt, Yukon, Canada: Economic Geology, v. 101, p. 523-553.

McCuaig, T. C., and Kerrich, R., 1998, P-T-t-deformation-fluid characteristics of lode gold deposits: evidence from alteration systematics: Ore Geology Reviews, v. 12, p. 381-453.

McNaughton, N. J., Cassidy, K., Groves, D. I., and Perring, C. S., 1990, Timing of mineralization, in Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold Deposits of the Yilgarn Block Western Australia: Nature, Genesis and Exploration Guides: Perth, Department of Geology and University Extension, University of Western Australia Publication No. 20, p. 221-225.

McNaughton, N. J., Groves, D. I., and Witt, W. K., 1993, The source of lead in Archaean lode gold deposits of the Menzies-Kalgoorlie-Kambalda region, Yilgarn Block, Western Australia: Mineralium Deposita, v. 28, p. 495-502.

McNaughton, N. J., Mueller, A. G., and Groves, D. I., 2005, The Age of the Giant Golden Mile Deposit, Kalgoorlie, Western Australia: Ion-Microprobe Zircon and Monazite U-Pb Geochronology of a Synmineralization Lamprophyre Dike: Economic Geology, v. 100, p. 1427-1440.

Mernagh, T., 1996, Gold mineralisation at Mount Charlotte: evidence for fluid oxidation from fluid inclusions: Geological Society of Australia, abstracts, v. 41, p. 292.

Mernagh, T. P., and Bierlein, F. P., 2008, Transport and Precipitation of Gold in Phanerozoic Metamorphic Terranes from Chemical Modeling of Fluid-Rock Interaction: Economic Geology, v. 103, p. 1613-1640.

Mikucki, E., and Groves, D. I., 1990, Nature of ore fluid, and transportational and depositional conditions in sub-amphibolite facies deposits: Mineralogical constraints, in Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold deposits of the

REFERENCES

205

Archean Yilgarn block, Western Australia: Nature, genesis and exploration guides: Perth, Geology Department (Key Centre) and University Extension, the University of Western Australia, Publication No. 20, p. 212-220.

Mikucki, E., and Heinrich, C. A., 1993, Vein- and mine-scale wall-rock alteration and gold mineralization in the Archaean Mount Charlotte Deposit, Kalgoorlie, Western Australia: Kalgoorlie '93 extended abstracts, Australian Geological Survey Organisation, Record 1993/54, p. 135-140.

Mikucki, E., and Ridley, J., 1993, The hydrothermal fluid of Archaean lode-gold deposits at different metamorphic grades: compositional constraints from ore and wallrock alteration assemblages: Mineralium Deposita, v. 28, p. 469.

Mikucki, E. J., 1998, Hydrothermal transport and depositional processes in Archean lode-gold systems: A review: Ore Geology Reviews, v. 13, p. 307.

Mikucki, E. J., 2000, Thermochemical models for ore-genesis and ore-fluid formation and evolution in the Golden Mile system: Part I. Role of fluid-rock reaction and pre-lode carbonation, AMIRA Project P511, p. 34

Mikucki, E. J., 2001, Thermochemical models for ore-genesis and ore-fluid evolution in Archean lode-gold systems: Follow-up on host-rock buffering of ore fluid oxidation states, AMIRA Project P511, p. 45.

Miller, J., Blewett, R., Tunjic, J., and Cassidy, K., 2009, The role of early formed structures on the development of the world-class St Ives gold camp, Yilgarn, WA: CET Quarterly News Letter, p. 1-7.

Moh, G. H., 1980, Ore syntheses, phase equilibria studies and applications: Neues Jahrbuch für Mineralogie. Abhandlungen, v. 139, p. 114-154.

Morey, A., 2007, Controls on gold endowment within the Bardoc Tectonic Zone, Eastern Goldfields Province, Western AustraliaAnthony: Unpub. PhD thesis, Monash University, 118 p.

Morey, A., Weinberg, R. F., and Bierlein, F., 2007, The structural controls of gold mineralization within the Bardoc Tectonic Zone, Eastern Goldfields Province, Western Australia: implications for gold endowments in shear systems: Mineralium Deposita, v. 42, p. 583-600.

Mueller, A. G., 2007, Copper-gold endoskarns and high-Mg monzodiorite-tonalite intrusions at Mt. Shea, Kalgoorlie, Australia: implications for the origins of gold-pyrite-tennantite mineralization in the Golden Mile: Mineralium Deposita, v. 42, p. 737-769.

Mueller, A. G., de Laeter, J. R., and Groves, D. I., 1991, Strontium Isotope Systematics of Hydrothermal Minerals from Epigenetic Archean Gold Deposits in the Yilgarn Block, Western Australia: Economic Geology, v. 86, p. 780-809.

Mueller, A. G., and Groves, D. I., 1991, The classification of Western Australian greenstone-hosted gold deposits accordeing to wallrock-alteration mineral assemblages: Ore Geology Reviews, v. 6, p. 291-331.

Mueller, A. G., Harris, L. B., and Lungan, A., 1988, Structural control of greenstone-hosted gold mineralization by transcurrent shearing: A new interpretation of the Kalgoorlie Mining District, Western Australia: Ore Geology Reviews, v. 3, p. 359-387.

Naden, J., and Shepherd, T. J., 1989, Role of methane and carbon dioxide in gold deposition: Nature, v. 342, p. 793-795.

Nelson, D. R., 1997, Evolution of the Archaean granite-greenstone terranes of the Eastern Goldfields, Western Australia: SHRIMP U-Pb zircon constraints: Precambrian Research, v. 83, p. 57-81.

Nesbitt, B. E., and Muehlenbachs, K., 1989, Geology, geochemistry and genesis of mesothermal lode gold deposits of the Canadian Cordillera: evidence for ore formation from evolved meteoric water. , in Keays, R. R., Ramsay, W. R. H.,

REFERENCES

206

and Groves, D. I., eds., The geology of gold deposits: The perspective in 1988, Economic Geology Monograph 6, p. 553-563.

Nesbitt, B. E., Murowchick, J. B., and Muehlenbachs, K., 1986, Dual origins of lode gold deposits in the Canadian Cordillera: Geology v. 14, p. 506-509.

Neumayr, P., and Hagemann, S. E., 2002, Hydrothermal fluid evolution within the Cadillac Tectonic Zone, Abitibi Greenstone Belt, Canada: Relationship to auriferous fluids in adjacent second- and third-order shear zones: Economic Geology, v. 97, p. 1203-1225.

Neumayr, P., Hagemann, S. E., Banks, D. A., Yardley, B. W. D., Couture, J. F., Landis, G. P., and Rye, R., 2007, Fluid Chemistry and Evolution of Hydrothermal Fluids in an Archaean Transcrustal Fault Zone Network: the Case of the Cadillac Tectonic Zone, Abitibi Greenstone Belt, Canada: Canadian Journal of Earth Sciences, v. 44, p. 745-773.

Neumayr, P., Hagemann, S. G., and Couture, J. F., 2000, Structural setting, textures, and timing of hydrothermal vein systems in the Val d'Or Camp, Abitibi, Canada; implications for the evolution of transcrustal, second- and third-order fault zones and gold mineralization: Canadian journal of earth sciences, v. 37, p. 95.

Neumayr, P., Petersen, K. J., Gauthier, L., Hodge, J. L., Hagemann, S. G., Walshe, J. L., Prendergast, K., Conners, K., Horn, L., Frikken, P., Roache, A., and Blewett, R., 2005, Mapping of hydrothermal alteration and geochemical gradients as a tool for conceptual targeting: St. Ives gold camp, Western Australia, in Mao J, B. F., ed., Mineral deposit research: meeting the global challenge. Proceedings of the Eighth Biennial SGA Meeting, Beijing: Heidelberg, Springer, p. 1479-1482.

Neumayr, P., Walshe, J. L., Connors, K., Cox, S. F., Morrison, R. S., and Stolz, E., 2004, Gold mineralization in the St Ives camp near Kambalda, in Neumayr, P., Harris, M., and Beresford, S. W., eds., Gold and nickel deposits in the Archaean Norseman-Wiluna greenstone belt, Yilgarn Craton, Western Australia - a field guide, Geological Survey of Western Australia, Record 2004/16, p. 23-45.

Neumayr, P., Walshe, J. L., Hagemann, S. G., Petersen, K. J., Roache, A., Frikken, P., Horn, L., and Halley, S., 2008, Oxidized and reduced mineral assemblages in greenstone belt rocks of the St. Ives gold camp, Western Australia: vectors to high-grade ore bodies in Archaean gold deposits? : Mineralium Deposita, v. 43, p. 363-371.

Nguyen, P. T., 1997, Structural controls on gold mineralization at the Revenge mine and its tectonic setting in the Lake Lefroy area, Kambalda, WA: Unpub. PhD thesis, University of Western Australia, 195 p.

Nguyen, P. T., Cox, S. F., Harris, L. B., and Powell, C. M., 1998, Fault-valve behaviour in optimally oriented shear zones: An example at the Revenge gold mine, Kambalda, Western Australia: Journal of Structural Geology, v. 20.

Nichols, S., 2003, Structural control, hydrothermal alteration and relative timing of gold mineralisation at the New Celebration gold deposits, Kalgoorlie, Western Australia: Unpub. BSc (Hons) thesis, University of Western Australia, 62 p.

Nichols, S. J., Hagemann, S. G., and Neumayr, P., in revision, Structural and hydrothermal alteration evidence for early and late stages of gold mineralisation at the New Celebration gold deposits in Western Australia.

Nichols, S. J., Hagemann, S. G., Neumayr, P., and Humphries, M., 2004, Structural control, hydrothermal alteration and relative timing of gold mineralisation at the Archaean New Celebration gold deposits, Kalgoorlie, Western Australia. , in McPhie, J., and McGoldrick, P., eds., Dynamic Earth; past, present and future. Abstracts - Geological Society of Australia, p. 105.

REFERENCES

207

Nickel, E. H., 1977, Mineralogy of the "green leader" gold ore at Kalgoorlie, Western Australia: Australasian Institute of Mining and Metallurgy, v. 263, p. 9-13.

Norris, N. D., 1990, New Celebration gold deposits, in Hughes, F. E., ed., Geology of the mineral deposits of Australia and Papua New Guinea, Melbourne, , Monograph 14, Australasian Institute of Mining and Metallurgy, p. 449-454.

Oberthuer, T., Mumm, A. S., Vetter, U., Simon, K., and Amanor, J. A., 1996, Gold mineralization in the Ashanti Belt of Ghana; genetic constraints of the stable isotope geochemistry: Economic Geology, v. 91, p. 289-301.

Ohmoto, H., 1986, Stable isotope geochemistry of ore deposits, in Valley, J. W., Taylor, H. P., and O'Neil, J. R., eds., Stable isotopes in high temperature geological processes, Mineralogical Society of America Reviews in Mineralogy v. 16

p. 491-560. Ohmoto, H., and Goldhaber, M. B., 1997, Sulfur and carbon isotopes, in Barnes, H. L.,

ed., Geochemistry of Hydrothermal Ore Deposits: New York, John Wiley and Sons, p. 517-612.

Ohmoto, H., and Rye, R., 1979, Isotopes of Sulphur and Carbon, in Barnes, H. L., ed., Geochemistry of Hydrothermal Ore Deposits: New York, Wiley, p. 509-567.

Ojala, J., 1995, Structural and depositional controls on gold mineralization at the Granny Smith Mine, Laverton, Western Australia: Unpub. PhD thesis, University of Western Australia, 184 p.

Ojala, J., Groves, D. I., and Ridley, J. R., 1995, Hydrogen isotope fractionation factors between hydrous minerals and ore fluids at low temperatures: evidence from the Granny Smith gold deposit, Western Australia: Mineralium Deposita, v. 30, p. 328-331.

Ojala, J., Ridley, J. R., Groves, D. I., and Hall, G. C., 1993, The Granny Smith gold deposit: the role of heterogeneous stress distribution at an irregular granitoid contact in a greenschist facies terrane: Mineralium Deposita, v. 28, p. 409-419.

Olivo, G. R., Chang, F., and Kyser, T. K., 2006, Formation of the auriferous and barren North Dipper veins in the Sigma mine, Val d'Or, Canada: Constraints from structural, mineralogical, fluid inclusion and isotopic data: Economic Geology, v. 101, p. 607-631.

Ozima, M., and Posodek, F. A., 2002, Noble Gas Geochemistry, Cambridge University Press, 300 p.

Palin, J. M., and Xu, Y., 2000, Gilt by Association? Origins of Pyritic Gold Ores in the Victory Mesothermal Gold Deposit, Western Australia: Economic Geology, v. 95, p. 1627-1634.

Pals, D., and Spry, P. G., 2003, Telluride mineralogy of the low-sulfidation epithermal Emperor gold deposit, Vatoukola, Fiji: Journal of Mineralogy and Petrology, v. 79, p. 285-307.

Partington, G. A., and Williams, P. J., 2000, Proterozoic lode gold and (iron)-copper-gold deposits: A comparison of Australian and global examples: Reviews in Economic Geology, v. 13, p. 69-101.

Passchier, C. W., 1994, Structural geology across a proposed terrane boundary in the eastern Yilgarn craton, Western Australia: Precambrian Research, v. 68, p. 43-64.

Passchier, C. W., and Trouw, R. A. J., 1996, Microtectonics, Springer. Petersen, K. J., Neumayr, P., Hagemann, S. G., and Walshe, J. L., 2005,

Paleohydrologic evolution of the St. Ives gold camp, in Mao, J., and Bierlein, F., eds., Mineral Deposit Research: Meeting the Global Challenge, Proceedings of the Eighth Biennial SGA Meeting, Beijing, China, 18-21 August 2005, p. 573-576.

REFERENCES

208

Petersen, K. J., Neumayr, P., Walshe, J. L., and Hagemann, S. G., 2006, Types of fluid compositions and evolution at the St Ives gold camp, in Anonymous, ed., Geochimica et Cosmochimica Acta, 70, p. A485.

Phillips, D., and Miller, J., 2006, 40Ar/39Ar dating of mica-bearing pyrite from thermally overprinted Archean gold deposits: Geology, v. 34, p. 397-400.

Phillips, G. N., 1986, Geology and alteration in the Golden Mile, Kalgoorlie: Economic Geology, v. 81, p. 779-808.

Phillips, G. N., and Groves, D. I., 1983, The nature of Archaean gold-bearing fluids as deduced from gold deposits of Western Australia: Geological Society of Australia Journal, v. 30, p. 25-39.

Phillips, G. N., Groves, D. I., Amaro, D., Hallbauer, D. K., and Fotios, M. G., 1988, Morphology and trace-element compositions of pyrites from Kalgoorlie gold deposits: sensitive indicators of syndeformational fluid regimes and depositional processes, in Ho, S. E., and Groves, D. I., eds., Advances in Understanding Precambrian Gold Deposits, Volume II: Perth, Geology Department and University Extension, the University of Western Australia, Publication 12, p. 217-226.

Phillips, G. N., Groves, D. I., and Brown, I. J., 1987, Source requirements for the Golden Mile, Kalgoorlie: Significance to the metamorphic replacement model for Archean gold deposits: Canadian Journal of Earth Sciences, v. 24, p. 1643-1651.

Phillips, G. N., Groves, D. I., and Kerrich, R., 1996, Factors in the formation of the giant Kalgoorlie gold deposit: Ore Geology Reviews, v. 10, p. 295.

Phillips, G. N., Groves, D. I., Neall, F. B., Donnelly, T. H., and Lambert, I. B., 1986, Anomalous sulfur isotope composition in the Golden Mile, Kalgoorlie: Economic Geology, v. 81, p. 2008-2015.

Pike, S., 1993, The chemistry of granite derived pegmatite fluids: Unpub. PhD thesis, University of Leeds, 244 p.

Pitcairn, I. K., Teagle, D. A. H., Craw, D., Olivo, G. R., Kerrich, R., and Brewer, T. S., 2006, Sources of Metals and Fluids in Orogenic Gold Deposits: Insights from the Otago and Alpine Schists, New Zealand: Economic Geology, v. 101, p. 1525-1546.

Polito, P. A., Bone, Y., Clarke, J. D. A., and Mernagh, T., 2001, Compositional zoning of fluid inclusions in the Archaean Junction gold deposit, Western Australia: a process of fluid-wall-rock interaction?: Australian Journal of Earth Sciences, v. 48, p. 833-855.

Powell, R., Will, T. M., and Phillips, G. N., 1991, Metamorphism in Archaean greenstone belts: Calculated fluid compositions for gold mineralization: Journal of Metamorphic Geology, v. 9, p. 141-150.

Pudack, C., Halter, W. E., Heinrich, C. A., and Pettke, T., 2009, Evolution of Magmatic Vapor to Gold-Rich Epithermal Liquid: The Porphyry to Epithermal Transition at Nevados de Famatina, Northwest Argentina: Economic Geology, v. 104, p. 449-477.

Qiu, Y., and McNaughton, N. J., 1999, Source of Pb in orogenic lode-gold mineralisation: Pb isotope constraints from deep crustal rocks from the southwestern Archaean Yilgarn Craton, Australia: Mineralium Deposita, v. 34, p. 366.

Quan, R. A., Cloke, P. L., and Kesler, S. E., 1987, Chemical analyses of halite trend inclusions from the Granisle porphyry copper deposit, British Columbia: Economic Geology, v. 82, p. 1912-1930.

REFERENCES

209

Ramboz, C., Pichavant, M., and Weisbrod, A., 1982, Fluid immiscibility in natural processes: Use and misuse of fluid inclusion data II. Interpretation of fluid inclusion data in terms of immiscibility: Chemical Geology, v. 37, p. 29-48.

Redmond, P. B., Einaudi, M. T., Inan, E. E., Landtwing, M. R., and Heinrich, C. A., 2004, Copper deposition by fluid cooling in intrusion-centered systems: New insights from the Bingham porphyry ore deposit, Utah: Geology, v. 32, p. 217-220.

Reed, M. H., 1998, Calculation of simultaneous chemical equilibria in aqueous-mineral-gas systems and its application to modeling hydrothermal processes, in Richards, J. P., and Larson, P. B., eds., Techniques in hydrothermal ore deposits geology, Reviews in Economic Geology v.10, p. 109-124.

Richards, J. P., and Kerrich, R., 1993, The Porgera gold mine, Papua New Guinea: Magmatic hydrothermal to epithermal evolution of an alkalic-type precious metal deposit: Economic Geology, v. 88, p. 1017-1052.

Ridley, J., and Mengler, F., 2000, Lithological and structural controls on the form and setting of vein stockwork orebodies at the Mount Charlotte gold deposit, Kalgoorlie: Economic Geology, v. 95, p. 85-98.

Ridley, J. R., and Diamond, L. W., 2000, Fluid chemistry of lode gold deposits, and implications for genetic models, in Hagemann, S. G., and Brown, P. E., eds., Gold in 2000, Reviews in Economic Geology, v. 13, p. 141-162.

Ridley, J. R., and Hagemann, S. G., 1996, Fluid inclusions in Archean high-temperature gold deposits; can we evaluate post-entrapment modification?, in Brown, P. E., and Hagemann, S. G., eds., PACROFI VI; Sixth biennial Pan-American conference on Research on fluid inclusions; program and abstracts, p. 104-106.

Robert, F., 1989, Internal structure of the Cadillac tectonic zone southeast of Val d'or, Abitibi greenstone belt, Quebec: Canadian Journal of Earth Sciences, v. 26, p. 2661-2675.

Robert, F., 1990, An overview of gold deposits in the eastern Abitibi subprovince: Canadian Institute of Mining and Metallurgy Special Volume, v. 43, p. 93-105.

Robert, F., and Kelly, W. C., 1987, Ore-forming fluids in Archean gold-bearing quartz veins at the Sigma Mine, Abitibi Greenstone Belt, Quebec, Canada: Economic Geology, v. 82, p. 1464-1482.

Robert, F., and Poulsen, K. H., 1997, World-class gold deposits in Canada: an overview: Australian Journal of Earth Sciences, v. 44, p. 329-351.

Robert, F., Poulsen, K. H., Cassidy, K., and Hodgson, C. J., 2005, Gold metallogeny of the Superior and Yilgarn cratons: economic Geology 100th Anniversary Volume, p. 1001-1033.

Roberts, R. G., 1988, Archean lode gold deposits, in Roberts, R. G., and Sheahan, P. A., eds., Ore Deposit Models, Reprint Series 3, Geoscience Canada, p. 1-19.

Robinson, B. W., and Kusakabe, M., 1975, Quantitative preparation of sulfur dioxide for 34S/32S analyses from sulfides by combustion with cuprous oxide: Analytical Chemistry, v. 47, p. 1179-1181.

Rock, N. M., 1990, Lamprophyres: Glascow, Blackies, 285 p. Rock, N. M., and Groves, D. I., 1988a, Can lamprophyres resolve the genetic

controversy over mesothermal gold deposits: Geology, v. 16, p. 538-541. Rock, N. M., and Groves, D. I., 1988b, Do lamprophyres carry gold as well as

diamonds?: Nature, v. 253, p. 253-255. Rock, N. M., Groves, D. I., Perring, C. S., and Golding, S. D., 1989, Gold,

lamprophyres and porphyries: what does their association mean?, in Keays, R. R., Ramsay, W. R. H., and Groves, D. I., eds., The Geology of Gold Deposits: The Perspective in 1988. Economic Geology Monograph 6, p. 609-625.

REFERENCES

210

Roedder, E., 1971, Fluid inclusion studies on the porphyry-type ore deposits at Bingham, Utah, Butte, Montana, and Climax, Colorado: Economic Geology, v. 66, p. 98-120.

Roedder, E., 1972, Compositions of fluid inclusions: US Geological Survey Professional Paper 440-JJ p. 1-64.

Roedder, E., 1979, Fluid inclusions as samples of ore fluids, in Barnes, H. L., ed., Geochemistry of Hydrothermal Ore Deposits, 2nd Edition: New York, Wiley, p. 684-737.

Roedder, E., 1984, Fluid Inclusions, Mineralogical Society of America, 644 p. Rosler, H. J., and Lange, H., 1972, Geochemical Tables: Amsterdam, Elsevier, 468 p. Rusk, B. G., Reed, M. H., Dilles, J. H., Klemm, L. M., and Heinrich, C. A., 2004,

Compositions of magmatic hydrothermal fluids determined by LA-ICP-MS of fluid inclusions from the porphyry copper-molybdenum deposit at Butte, MT: Chemical Geology, v. 210, p. 173-199.

Scantlebury, G. M., 1983, The characterization and origin of the gold lodes in and around the Brownhill syncline, Golden Mile, Kalgoorlie, Western Australia: Unpub. BSc (Honours) thesis, University of Western Australia, 90 p.

Schiller, J. C., and Ivey, M. E., 1990, Hannan South gold deposit, in Hughes, F. E., ed., Geology of the Mineral Deposits of Australia and Papua New Guinea, The Australasian Institute of Mining and Metallurgy, Melbourne, p. 443-447.

Seccombe, P. K., Groves, D. I., Marston, R. J., and Barrett, F. M., 1981, Sulfide paragenesis and sulfur mobility in Fe-Ni-Cu sulfide ores at Lunnon and Juan Main Shoots, Kambalda: Textural and sulfur isotopic evidence: Economic Geology, v. 76, p. 1675-1685.

Seward, T. M., 1973, Thio complexes of gold and the transport of gold in hydrothermal ore solutions: Geochimica et Cosmochimica Acta, v. 37, p. 379.

Seward, T. M., 1984, The transport and deposition of gold in hydrothermal systems, in Foster, R. P., ed., Gold '82: The Geology, Geochemistry and Genesis of Gold Deposits: Rotterdam, A.A. Balkema, p. 165-182.

Shackleton, J. M., Spry, P. G., and Bateman, R. J., 2003, Telluride mineralogy of the Golden Mile deposit, Kalgoorlie, Western Australia: Canadian Mineralogist, v. 41, p. 1503-1524.

Shepherd, T. J., Rankin, A. H., and Alderton, D. H. M., 1985, A practical guide to fluid inclusion studies: Glasgow, Blackie, 239 p.

Sibson, R. H., 2001, Seismogenic framework for hydrothermal transport and ore deposition, in Richards, J. P., and Tosdal, R. M., eds., Structural Controls on Ore Genesis, SEG Reviews, v. 14, p. 25-50.

Sibson, R. H., 2004, Controls on maximum fluid overpressure defining conditions for mesozonal mineralisation: Journal of Structural Geology, v. 26, p. 1127-1136.

Sibson, R. H., Robert, F., and Poulsen, K. H., 1988, High angle reverse faults, fluid-pressure cycling, and mesothermal gold-quartz deposits: Geology v. 16, p. 551-555.

Simmons, S. F., Sawkins, F. J., and Schlutter, D. J., 1987, Mantle derived helium in two Peruvian hydrothermal ore deposits: Nature, v. 329, p. 429-432.

Smith, J. R., Spooner, E. T. C., Broughton, D. W., and Ploeger, F. R., 1993, Archean Au-Ag-(W) Quartz Vein/Disseminated mineralisation within the Larder Lake - Cadillac Break, Kerr Addison - Chesterville System, North East Ontario, Canada, Ontario Geoscience Research Grant Program, Grant No. 364; Ontario Geological Survey, Open File Report 5831, p. 310.

Sorby, H. C., 1858, On the microscopical structure of crystals indication the origin of rocks and minerals: Quarterly Journal of the Geological Society of London, v. 14, p. 453-500.

REFERENCES

211

Stolz, E., Urosevic, M., and Connors, K., 2004, Reflection seismic surveys at St Ives Gold Mine, WA, in Australian Society of Exploration Geophysicists, P., Western Australia, Australia, Petroleum Exploration Society of Australia, Sydney, N.S.W., Australia ed., Integrated exploration in a changing world; 17th ASEG-PESA geophysical conference and exhibition; extended abstracts.

Stuwe, K., Will, T. M., and Zhou, S., 1993, On the timing relationship between fluid production and metamorphism in metamorphic piles: some implications for the origin of post-metamorphic gold mineralization: Earth and Planetary Science Letters, v. 114, p. 417-430.

Swager, C., 1989, Structure of Kalgoorlie greenstones - regional deformation history and implications for the structural setting of the Golden Mile gold deposits, Geological Society of Western Australia Report 25, p. 59-84.

Swager, C., 1997, Tectono-stratigraphy of late Archaean greenstone terranes in the southern Eastern Goldfields, Western Australia: Precambrian Research, v. 83, p. 11-42.

Swager, C., and Griffin, T. J., 1990, Geology of the Archaean Kalgoorlie Terrane (northern and southern sheets), Western Australian Geological Survey, 1:250,000 Geological Map.

Swager, C., Griffin, T. J., Witt, W. K., Wyche, S., Ahmat, A. L., Hunter, W. M., and McGoldrick, P. J., 1995, Geology of the Archean Kalgoorlie Terrane - an explanatory note, 26 p.

Swager, C., and Nelson, D. R., 1997, Extensional emplacement of a high-grade granite gneiss complex into low-grade greenstones, Eastern Goldfields, Yilgarn Craton, Western Australia: Precambrian Research, v. 83, p. 203-219.

Swager, C. P., Goleby, B. R., Drummond, B. J., Rattenbury, M. S., and Williams, P. R., 1997, Crustal structure of granite-greenstone terranes in the Eastern Goldfields, Yilgarn Craton, as revealed by seismic reflection profiling: Precambrian Research, v. 83, p. 43.

Swager, C. P., Witt, W. K., Griffin, T. J., Ahmat, A. L., Hunter, W. M., McGoldrick, P. J., and Wyche, S., 1992, Late Archaean granite-greenstones of the Kalgoorlie Terrane, Yilgarn Craton, Western Australia, in Glover, J. E., and Ho, S. E., eds., The Archaean: Terrains, processes and Metallogeny, Geology Department (Key Centre) and University Extension, the University of Western Australia, Publication No. 22, p. 107-122.

Swanenberg, H. E. C., 1979, Phase equilibria in carbonic systems, and their application to freezing studies of fluid inclusions: Contributions to Mineralogy and Petrology, v. 68, p. 303-306.

Szumigala, D. J., Dodd, S. L., and Arribas, A. P., 2000, Geology and gold mineralization at the Donlin Creek prospects, southwest Alaska, in Pinney, D. S., ed., Short Notes on Alaskan Geology, Alaska Division of Geological and Geophysical Surveys Professional Report, p. 104-122.

Takenouchi, S., and Kennedy, G. C., 1965, The solubility of carbon dioxide in NaCl solutions at high temperatures and pressures: American Journal of Science, v. 263, p. 445-454.

Taylor, B. E., Robert, F., Ball, M., and Leitch, C. H. B., 1991, Mesozoic "Mother Lode Type" gold deposits in North America: Primary vs. secondary (meteoric) fluids (abs): Geological Society of America Abstracts with Programs, v. 23(6), p. 174.

Taylor, H. P., Kesler, S. E., Cloke, P. L., and Kelly, W. C., 1983, Fluid inclusion evidence for fluid mixing, Mascot-Jefferson City zinc district, Tennessee: Economic Geology, v. 78, p. 1425-1439.

Taylor, S. R., 1964, Chondritic earth model: Nature, v. 202, p. 281-282.

REFERENCES

212

Thébaud, N., Philippot, P., Rey, P., and Cauzid, J., 2006, Composition and origin of fluids associated with lode gold deposits in a Mesoarchean greenstone belt (Warrawoona Syncline, Pilbara Craton, Western Australia) using synchrotron radiation X-ray fluorescence: Contributions to Mineralogy and Petrology, v. 152, p. 485-503

Thiery, R., van den Kerkhof, A. M., and Dubessy, J., 1994, vX properties modeling of CH4-CO2 and CO2-N2 fluid inclusions (T<31°C, P<400 bar): European Journal of Mineralogy, v. 6, p. 753-771.

Thode, H. G., Ding, T., and Crockett, J. H., 1991, Sulphur-isotope and elemental geochemistry studies of the Hemlo gold mineralization, Ontario: sources of sulphur and implications for the mineralization process: Canadian Journal of Earth Sciences, v. 28, p. 13-25.

Thompson, J. F. H., and Newberry, R. J., 2000, Gold deposits related to reduced granitic intrusions: SEG Reviews, v. 13, p. 377-400.

Thompson, J. F. H., Sillitoe, R. H., Baker, T., Lang, J. R., and Mortensen, J. K., 1999, Intrusion-related gold deposits associated with tungsten-tin provinces: Mineralium deposita, v. 34, p. 323.

Thompson, T. B., 1998, Cripple Creek, a world-class gold-bearing diatreme-alkalic complex, Colorado, USA: Geological Society of America Abstracts with Programs, v. 30, p. 301.

Townsend, D. B., Mai, G., and Morgan, W. R., 2000, Mines and mineral deposits of Western Australia: digital extract from MINEDEX - an explanatory note, Geological Survey of Western Australia, Record 2000/13, p. 28.

Uemoto, T., Ridley, J., Mikucki, E., Groves, D. I., and Kusakabe, M., 2002, Fluid Chemical Evolution as a Factor in Controlling the Distribution of Gold at the Archean Golden Crown Lode Gold Deposit, Murchison Province, Western Australia: Economic Geology, v. 97, p. 1227-1248.

Ulrich, T., and Gunther, D., 2002, The Evolution of a Porphyry Cu-Au Deposit, Based on LA-ICP-MS Analysis of Fluid Inclusions: Bajo de la Alumbrera, Argentina: Economic Geology, v. 97, p. 1889-1920.

Ulrich, T., Gunther, D., and Heinrich, C. A., 1999, Gold concentrations of magmatic brines and the metal budget of porphyry copper deposits: Nature, v. 399, p. 676.

Walshe, J. L., Neumayr, P., and Petersen, K. J., 2006, Scale-integrated, architectural and geodynamic controls on alteration and geochemistry of gold systems in the Eastern Goldfields Province, Yilgarn Craton, Final Report 256, Minerals and Energy Research Institute of Western Australia, p. 289.

Watchorn, R. B., 1998, Kambalda-St Ives gold deposits, in Berkman, D. A., and McKenzie, D. H., eds., Geology of Australia and Papua New Guinea mineral deposits, Monograph Series, 22, Australasian Institute of Mining and Metallurgy, p. 243-254.

Weinberg, R. F., Moresi, L., and van der Borgh, P., 2003, Timing of deformation in the Norseman-Wiluna Belt, Yilgarn Craton, Western Australia: Precambrian Research, v. 120, p. 219-239.

Weinberg, R. F., Van der Borgh, P., Bateman, R. J., and Groves, D. I., 2005, Kinematic History of the Boulder-Lefroy Shear Zone System and Controls on Associated Gold Mineralization, Yilgarn Craton, Western Australia: Economic Geology, v. 100, p. 1407-1426.

Whitney, J. A., Hemley, J. J., and Simon, F. O., 1985, Fluid inclusion geochemistry of the Granisle and Bell porphyry copper deposits, British Columbia: Economic Geology, v. 75, p. 45-61.

Wilkinson, J. J., 2001, Fluid inclusions in hydrothermal ore deposits: Lithos, v. 55, p. 229-272.

REFERENCES

213

Wilkinson, L., Cruden, A. R., and Krogh, T. E., 1999, Timing and kinematics of post-Timiskaming deformation within the Larder Lake-Cadillac deformation zone, southwest Abitibi greenstone belt, Ontario, Canada: Canadian Journal of Earth Sciences, v. 36, p. 627-647.

Williams-Jones, A. E., and Heinrich, C. A., 2005, 100th Anniversary Special Paper: Vapor Transport of Metals and the Formation of Magmatic-Hydrothermal Ore Deposits: Economic Geology, v. 100, p. 1287-1312.

Williams, H., 1994, The lithological setting and controls on gold mineralization in the Southern Ore Zone of the Hampton-Boulder gold deposit, New Celebration Gold Mine, Western Australia: Unpub. BSc (Hons) thesis, University of Western Australia.

Williams, P. R., and Currie, K. L., 1993, Character and regional implication of the sheared Archaean granite-greenstone contact near Leonora, Western Australia: Precambrian Research, v. 62, p. 343-365.

Williams, T., 1991, A structural and lithological investigation of the Jubilee gold mine with particular attention to fault structures: Unpub. BSc (Hons) thesis, Western Australian School of Mines.

Wilson, J. W. J., Kesler, S. E., Cloke, P. L., and Kelly, W. C., 1980, Fluid inclusion geochemistry of the Granisle and Bell porphyry copper deposits, British Columbia: Economic Geology, v. 75, p. 45-61.

Witt, W. K., 1991, Regional metamorphic controls on alteration associated with gold mineralization in the Eastern Goldfields province, Western Australia: Implications for the timing and origin of Archean lode-gold deposits: Geology, v. 19, p. 982-985.

Witt, W. K., 1993a, Gold deposits of the Kalgoorlie-Kambalda-St Ives area, Western Australia: Part 3 of a systematic study of the gold mines of the Menzies-Kambalda region, Geological Survey of Western Australia Record 1992/15, 108 p.

Witt, W. K., 1993b, Lithological and structural controls on gold mineralization in the Archaean Menzies-Kambalda area, Western Australia: Australian Journal of Earth Sciences, v. 40, p. 65-86.

Witt, W. K., and Swager, C., 1989, Structural setting and geochemistry of Archaean I-type granites in the Bardoc-Coolgardie area of the Norseman Wiluna belt, Western Australia: Precambrian Research, v. 44, p. 323-351.

Witt, W. K., and Vanderhor, F., 1998, Diversity within a unified model for Archaean gold mineralization in the Yilgarn Craton of Western Australia: An overview of the late-orogenic, structurally-controlled gold deposits: Ore Geology Reviews, v. 13, p. 29-64.

Wood, P. C., Burrows, D. R., Thomas, A. V., and Spooner, E. T. C., 1986, The Hollinger-McIntyre Au-quartz vein system, Timmins, Ontario, Canada; geologic characteristics, fluid properties and light stable isotope geochemistry, in Macdonald, A. J., ed., Gold '86, an International Symposium on the Geology of Gold Deposits: Toronto, p. 56-80.

Wood, S. A., and Samson, I. M., 1998, Solubility of ore minerals and complexation of ore metals in hydrothermal solutions, in Richards, J. P., and Larson, P. B., eds., Techniques in hydrothermal ore deposits geology, Reviews in Economic Geology v. 10, p. 33-80.

Woodall, R. W., 1965, Structure of the Kalgoorlie goldfield, in McAndrew, J., ed., Geology of Australian ore deposits. Second Edition: Melbourne, Eightth Emporial Mining and Metallurgical Congress, p. 71-79.

REFERENCES

214

Wopenka, B., and Pasteris, J. D., 1987, Raman intensities and detection limits of geochemically relevant gas mixtures for a laser Raman microprobe: Analytical Chemistry, v. 59, p. 2165-2170.

Yardley, B. W. D., 2005, Metal concentrations in crustal fluids and their relationship to ore formation: Economic Geology, v. 100, p. 613-632.

Yardley, B. W. D., Banks, D. A., Bottrell, S. H., and Diamond, L. W., 1993, Postmetamorphic gold-quartz veins from N.W. Italy: The composition and origin of the ore fluid: Mineralogical Magazine, v. 57, p. 407-422.

Yeats, C. J., Kohler, E. A., McNaughton, N. J., and Tkatchyk, L. J., 2001, SHRIMP U-Pb geochronological constraints on Archean volcanic-hosted massive sulfide and lode gold mineralization at Mount Gibson, Yilgarn craton, Western Australia: Economic Geology, v. 91, p. 1354-1371.

Zhang, X., and Spry, P. G., 1994, Petrological, mineralogical, fluid inclusion and stable isotope studies of the Gies gold-silver-telluride deposit, Judith Mountains, Montana: Economic Geology, v. 89, p. 602-627.

APPENDICES

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APPENDIX 1: “The New Celebration Gold Deposits: P-T-X Fluid

Evolution and Two Stages of Gold Mineralization within the Crustal-scale Boulder-Lefroy Shear Zone, Yilgarn

Craton, Western Australia”

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The New Celebration Gold Deposits: P-T-X Fluid Evolution and Two Stages of Gold Mineralization within the Crustal-scale Boulder-Lefroy Shear Zone, Yilgarn Craton, Western Australia Joanna L. Hodge1*, Steffen G. Hagemann1, Peter Neumayr1, Garry Davidson2 and David Banks3

1Centre for Exploration Targeting School of Earth and Environment University of Western Australia 35 Stirling Highway Crawley, WA 6009 AUSTRALIA 2CODES/Department of Earth Sciences University of Tasmania Private Bag 79 Hobart, TAS 7001, Australia 3School of Earth and Environment University of Leeds Leeds, LS2 9JT United Kingdom Corresponding author: e-mail [email protected] * Present address: Copper Ridge Explorations Incorporated 500-625 Howe Street, Vancouver, BC V6C 2T6, Canada

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Abstract

The western segment of the first-order, crustal scale Boulder-Lefroy fault zone hosts the

Archean New Celebration orogenic lode gold deposits. This setting contrasts with the majority of

orogenic lode gold deposits worldwide, which are typically located in higher order splays. Gold

mineralization took place in two stages at New Celebration: Stage I, which is related to ductile, sinistral

oblique slip fault movement and Stage II, which is related to brittle-ductile and brittle strike-slip fault

movement.

Quartz and quartz-calcite shear and extension veins concomitant with Stage I gold

mineralization contain primary and pseudo-secondary 2- and 3-phase aqueous-carbonic inclusions with

salinities between 2 and 8 wt percent (NaCl equiv), which homogenized to liquid or decrepitated via

expansion of the vapor phase between 226°C and 350°C. Pressure-temperature estimates indicate that

these inclusions were trapped between 300 and 500°C and 2.5 and 4.2 kilobars. Mixed aqueous-

carbonic inclusions with variable phase ratios and salinities of 1.8 to 7.7 weight percent (NaCl

equivalent) trapped in quartz-sericite-pyrite and quartz-calcite-pyrite veins associated with Stage II

gold mineralization typically homogenized or decrepitated between 250 and 300°C. Co-existing

aqueous>>carbonic inclusions with apparent maximum salinities between 0.8 and 9.3 weight percent

(NaCl equivalent) homogenized or decrepitated to liquid between 140 and 267°C. Pressure-temperature

estimates indicate that the Stage II gold-related fluids were trapped between 280 and 360°C and 1.5 to

3.5 kilobars, lower than the formation conditions of Stage I gold. Highly variable phase ratios, variable

bulk compositions and molar volumes of inclusions within the same trail or cluster and total

homogenization into liquid or vapor at the same temperature indicate that entrapment occurred during

phase separation. Secondary high-salinity (18.4 to 23.3 weight percent NaCl equivalent) aqueous

inclusions, trapped in both the Stage I and Stage II-related veins, invariably homogenized to liquid

below 100°C and along with secondary methane inclusions, were trapped between 80 and 250°C and

pressures around 1 kilobar.

Single inclusion laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS)

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analyses on aqueous and aqueous-carbonic inclusions indicate that the Stage I gold related fluids were

Ca dominant and contained lower concentrations of K, Mg, Cu, Pb, Zn, As, Sn and W than Stage II

fluids, which were Mg-K dominant. The K/Ca ratios vary by an order of magnitude between the two

mineralizing stages. This potentially indicates different K-Ca fluid sources for each mineralizing event

and suggests that a switch occurred in fluid and/or metal sources between Stage I and Stage II, possibly

from a metamorphic to a magmatic source.

Sulfur δ34S isotope ratios in ore-stage pyrite range between -7.6 per mil and +3.8 per mil from

Stage I mineralization, and between -10.6 per mil and -3.2 per mil from Stage II mineralization. These

values are predominantly within the documented range for orogenic lode gold deposits worldwide,

although the lightest values are amongst the most depleted values reported. In situ oxidation of the ore

fluid is discounted for Stage I mineralization therefore the isotopic composition of the ore stage pyrites

reflects the redox state of the ore-forming fluids. The depleted values of Stage II ore-related pyrite and

the spread of observed values is attributed to fluid oxidation during phase separation.

Pressure-temperature estimates describe an anticlockwise path and indicate that Stage I gold

mineralization occurred at temperatures and pressures similar to peak regional metamorphism, whereas

Stage II gold formed at lower temperatures and fluctuating pressures, likely during a period of uplift,

erosion and fault movement. Pyrite-magnetite and pyrite-gold petrography suggest that sulfidation

reactions with Fe-oxides were the main cause of gold mineralization in both mineralizing stages and

the sole cause of gold mineralization during Stage I. Fluid inclusion evidence suggests that phase

separation contributed to Stage II gold formation. The variety of fluids recorded within the BLFZ and

their diverse formation conditions suggest that the BLFZ was the main conduit for gold-related and

unrelated fluids in the region over a protracted period. Further, it appears that during the evolution of

the BLFZ it tapped at least two geochemically distinct crustal fluid reservoirs, which led to the

development of two gold mineralization stages at New Celebration with differing geochemical

characteristics.

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Introduction The Boulder-Lefroy fault zone (BLFZ) is an interpreted crustal-scale fault zone (e.g. Swager,

1989) located on the eastern margin of the Kalgoorlie Terrane (Fig. 1) in the Eastern Goldfields

Province of the Yilgarn craton, Western Australia. The BLFZ hosts the New Celebration gold deposits,

and is spatially correlated with the world-class Golden Mile and St Ives gold camps, both of which are

hosted in adjacent second- and third-order splays. Archean orogenic lode-gold camps world wide

typically show a close spatial correlation with first-order crustal scale fault zones (Eisenlohr et al.,

1989; Neumayr et al., 2000). In detail, however, higher-order splays host the majority of world class

(>100t Au) gold deposits (Eisenlohr et al., 1989; Groves et al., 1990). Much research into the P-T-X

evolution of the gold-endowed second- and third-order systems has been undertaken; however, only

sparse research is available on first-order structures. This is partly because most first-order systems are

barren and research has focused on the adjacent gold mineralized higher-order systems, but is also due

to the poor exposure of crustal scale structures worldwide. Recent work on first-order systems has

focused on the structure (Robert, 1989; Wilkinson et al., 1999), timing of mineralization (Robert, 1990;

Neumayr et al., 2000), hydrothermal fluid evolution (Neumayr and Hagemann, 2002) and tectonic

evolution (Neumayr et al., 2007) of the Cadillac Tectonic Zone in the Abitibi greenstone belt but there

has been very little research on similar structures in the Yilgarn craton.

The New Celebration gold deposits comprise six open pits (Hampton-Boulder, Jubilee,

Mutooroo, Celebration, Golden Hope and Early Bird) and the Hampton Decline underground operation

comprising four ore zones (Southern, Central, Northern and B40). Collectively the deposits produced

approximately 1.5 million ounces of gold between 1987 and 1997, with the majority of the gold coming

from the Hampton-Boulder (7.4Mt @ 2.34 g/t Au for 560,000 oz) and Jubilee (10.3Mt @ 2.09 g/t Au

for 1,325,000 oz) open pit deposits. These two deposits, which now comprise a single resource under

the ownership of Dioro Exploration NL are the focus of this study.

Previous workers at New Celebration have focused on the structural (Dielemans, 2000) and

lithological controls (Williams, 1994) of the Southern Ore Zone, whereas more recently Nichols

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(2003), Nichols et al. (2004) and Nichols et al. (in revision) evaluated the structural controls,

hydrothermal alteration and timing of gold mineralization of the New Celebration gold deposits.

Weinberg et al. (2005), evaluated the kinematic history of the BLFZ, whereas Hodkiewicz (2003)

evaluated the sulfur isotopic composition of ore-related sulfides from a number of Yilgarn deposits,

including those at New Celebration, as part of a more regional Yilgarn-scale study.

Orogenic gold deposits hosted in first-order fault systems are rare, therefore, the New

Celebration gold deposits provides a unique opportunity to study the fluid pressure-temperature-

composition (P-T-X) evolution, evaluate the role regional scale structures play in focusing mineralizing

and non-mineralizing fluids and potentially determine the source, or sources of fault zone fluids. This

paper builds on the structural and hydrothermal alteration assessments of Nichols (2003), Nichols et al.

(2004) and Nichols et al. (in revision) and presents the results of detailed petrographic, fluid inclusion,

stable isotope and LA-ICP-MS studies into the nature, composition, timing and source of fault zone

fluids in the BLFZ at the New Celebration deposits.

Geology of the Kalgoorlie Terrane The Kalgoorlie Terrane (Fig. 1) is a 6-9 kilometer thick, elongate, NNW trending volcano-

sedimentary sequence which is bounded to the east and west by wide (up to 1km) anastamosing shear

zones (Swager, 1997). The volcano-sedimentary greenstone belt sequence comprises basalt, komatiite

and felsic volcanic and volcaniclastic rocks, as well as a number of different granitoid suites. Coarse

clastic basin sequences, which unconformably overlie the greenstone belt sequence and commonly

bury major boundary faults are the youngest rocks (Swager, 1997). Regionally the terrane is

metamorphosed to upper greenschist facies, with locally higher metamorphic grades (up to amphibolite

facies) recorded along the margins of, and adjacent to granitoid plutons (Witt, 1991). Swager and

Nelson (1997) recognized four main compressive deformation episodes (D1-D4) in the Kalgoorlie

Terrane, each preceded by extensional periods. The volcano-sedimentary sequence was deposited

during the earliest extensional phase (Williams and Currie, 1993; Passchier, 1994) and was followed by

D1, a period of south over north compression, which occurred > 2675 Ma and resulted in widespread

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structural repetition and thrust faulting (Swager and Nelson, 1997). A second extensional phase

followed in which the coarse clastic sequences were deposited and widespread granitoid intrusion took

place (Weinberg et al., 2003). Regional D2 shortening at around 2675-2657 Ma (Nelson, 1997) was

approximately E-W and resulted in NNW-SSE trending upright folds and penetrative foliation

(Swager, 1989; Swager and Griffin, 1990; Weinberg et al., 2003). During D3 (2663-2645 Ma) and D4

(<2640 Ma) (Nelson, 1997; Swager, 1997), deformation became strike-slip in nature and progressed

from a ductile to a brittle regime (Mueller et al., 1988; Bateman et al., 2001)..

At New Celebration, the BLFZ occupies the hinge of the Celebration Anticline and has a

complicated history with a number of different interpretations regarding its movement sense. Swager

(1989) described it as a major oblique sinistral wrench structure, whereas several other authors inferred

reverse movement based on seismic data (Goleby et al., 2000) and field observations (Boulter et al.,

1987; Copeland, 1998; Ridley and Mengler, 2000), and dextral movement (Mueller et al., 1988). Most

recently, Weinberg et al. (2005) described the BLFZ as having formed by earlier thrust ramps linked

during sinistral strike-slip movement.

There are a number of reasons for the controversy surrounding the kinematic history of the

BLFZ. The fault is large, with a strike length extending over 200km, and in places the fault trace is

poorly defined. Outcrop is poor and there are only limited exposures where observations can be taken

directly from within the fault. In addition, the fault has been active with a number of different

movement senses throughout orogenesis, and therefore has had a long-lived and complex

deformational history. These factors have led to a number of discrepancies between authors when

describing the kinematic history of the shear system.

Geological Setting of the New Celebration Gold Deposits Previous workers have studied the geology, structural evolution and hydrothermal alteration of

the New Celebration deposits. The following section summarizes the geological descriptions of

Langsford (1989), Norris (1990), Williams (1994), Copeland (1998), Nichols (2003), Nichols et al.

(2004) and Nichols et al. (in revision) and the observations made during this study.

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Lithostratigraphy, deformation and magmatism

The New Celebration gold deposits are hosted within a sequence of folded and sheared

komatiites, differentiated dolerites and felsic volcaniclastic rocks, which have been intruded by several

generations of felsic and lamprophyric dikes and truncated by the BLFZ (Fig. 2). Regionally, the

sequence is metamorphosed to upper greenschist facies (Norris, 1990), although for simplicity the

prefix meta- is omitted from the geological descriptions in this paper. Gold mineralization is located

within or immediately adjacent to the shear zone (Norris, 1990; Copeland, 1998), in the hanging wall

of a steeply dipping, deformed contact between mafic and ultramafic rocks, within mafic schist, and

within and adjacent to strongly foliated to mylonitic intermediate plagioclase and felsic quartz-feldspar

porphyry dikes that intruded the contact along the BLFZ (Williams, 1994, Fig. 2a, 2b).

Nichols (2003) identified three main deformation events at New Celebration, and tentatively

correlated them with regional deformation events. For clarity Nichols (2003) identified the local New

Celebration events with the subscript NC; this convention is maintained throughout the manuscript. An

event correlating to regional D1 was not recognized at the New Celebration gold deposits. The earliest

recognized deformation event is D2NC, which is characterized by conformable stratigraphic contacts

that have been tilted to vertical. This event corresponds to the regional D2 upright folding of Swager

(1989) and Swager and Griffin (1990). The NW trending S-C fabrics (350/82W and 309/87W,

respectively), SSW-plunging mineral elongation lineations and sigmoidal quartz grains constrain

movement on the BLFZ during D3NC as sinistral oblique slip, west block down to the southwest

(Nichols, 2003; Nichols et al., 2004). This tentatively correlates with regional D3 ENE-WSW

compression and sinistral strike- and dip-slip faulting (Swager, 1989; Swager and Griffin, 1990).

Northwest dipping structures and a second penetrative S-C fabric (042/81W, 012/58W), which crosscut

S3NC, represent D4NC and constrain fault movement during D4NC as sinistral strike slip. Late

curviplanar faults that crosscut all other structures are assigned to D4+NC.

Nichols (2003) recognized two major magmatic events at New Celebration, based on

mineralogy, deformation style and crosscutting relationships. Early intensely carbonate-biotite-

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magnetite altered plagioclase porphyry dikes are denoted M1 and have a penetrative S3NC foliation.

These intrusions are crosscut by weakly albite-carbonate-magnetite-hematite altered, unfoliated to

weakly foliated quartz-feldspar porphyry dikes, designated M2, which preserve primary porphyritic

igneous textures. The M2 porphyries are boudinaged along strike and down dip, within the S3NC

foliation.

Ore bodies, hydrothermal alteration and gold mineralization

Mafic schists, mylonites and sheared intermediate porphyritic intrusions and felsic porphyries

host gold mineralization within brittle-ductile shear zones and quartz breccias (Williams, 1994;

Nichols, 2003). Ore zones are located in the hanging wall of a steeply dipping, deformed contact

between mafic and ultramafic rocks, and are spatially associated with, and hosted within, intermediate

and quartz-feldspar porphyry dikes that intruded the contact along the BLFZ (Williams, 1994). Nichols

(2003) identified two mineralizing events, Stage I and Stage II, and four mineralization styles classified

according to their mode of occurrence and host rocks. Stage I gold mineralization is associated with

ductile deformation and is hosted within fine-grained, deformed pyrite along foliation planes in

mylonitized and deformed intermediate M1 porphyry and mafic schists. Stage II is associated with

brittle-ductile deformation and hosted within high magnesium basalt and felsic porphyry that cross-cut

and intrude Stage I-hosting M1 porphyries, indicating that the mineralization events are separated in

time, although the absolute dates are unconstrained.

Stage I gold occurs as rounded inclusions within disseminated and deformed fine grained pyrite

aligned parallel to the S3NC foliation planes (Fig. 3) in mafic schists and strongly foliated to mylonitic

M1 porphyry, or within syn-D3NC quartz-calcite-pyrite veins. Ankerite and hydrothermal quartz

pressure shadows developed on the margins of the host pyrite within the foliation planes indicate that

pyrite and gold precipitated synchronous with D3NC deformation. Biotite-ankerite-albite-sericite-pyrite

alteration and a strong telluride association characterize Stage I gold mineralization. Pyrite replaces

pre-existing magnetite alteration, and in addition to gold inclusions contains rare (<1%) magnetite,

hematite, galena, chalcopyrite and pyrrhotite inclusions. Stage I is the significant gold event in terms of

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grade (4.7g/t Au) and tonnage (84.5 Mt) at New Celebration.

Stage II gold occurs as intragranular inclusions or along grain boundaries within pyrite at the

contact between high-Mg basalt and M2 quartz-feldspar porphyry and in pyrite within quartz-sericite-

pyrite veins developed on the margins of the felsic porphyry (Fig. 3). In contrast to Stage I, Stage II

gold-hosting pyrite is coarse-grained, predominantly euhedral, and where it is located at the mafic-

felsic contact, overprints the S3NC foliation, which wraps around the felsic porphyry (Fig. 3). The

proximal alteration assemblage to mineralization comprises ankerite-sericite-quartz±chlorite. Pyrite

abundance and gold concentration increases with proximity to the mafic-felsic contact. Tellurides were

not observed in Stage II gold mineralization. The location of Stage II gold mineralization within and

associated with undeformed M2 porphyries, which crosscut Stage I gold-hosting M1 porphyries, and

the location of gold in euhedral pyrite that overprints the S3NC foliation, indicate that Stage II post-

dates Stage I and is therefore interpreted to have occurred post-D3NC. Stage II gold mineralization is

characterized by lower gold grades (1.8g/t Au) and tonnage (10.4 Mt) when compared to Stage I gold

mineralization.

Vein Paragenesis

Vein types

Four major vein groups, correlated with specific deformation events and gold mineralization

styles, were identified at New Celebration (Fig. 4, Table 1). Type 1 quartz-calcite boudinaged veins

formed prior to D3NC and predate gold mineralization. Type 2 quartz±calcite veins developed during

D3NC and are synchronous with Stage I gold mineralization. Type 3 quartz breccia veins developed

during late D3NC or post D3NC and crosscut Stage I gold mineralization. Type 4 sericite-pyrite veins

developed during late D3NC or D4NC and host Stage II gold mineralization.

Vein mineralogy

The earliest observed Type 1 veins are foliation-parallel, quartz-calcite boudinaged veins,

which are situated in mylonites and strongly foliated M1 plagioclase porphyries (Fig. 4a). Quartz and

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calcite grains within these veins exhibit undulose extinction and have undergone complete dynamic

recrystallization by grain boundary migration and sub-grain rotation (c.f. Passchier and Trouw, 1996).

Type 2 veins comprise predominantly quartz-calcite± pyrite±ankerite and occur either parallel

or perpendicular to S3NC foliation. The veins that are located perpendicular to foliation show mutually

crosscutting relationships with the foliation planes (Fig. 4b) and are interpreted to have occurred

synchronous with S3NC and therefore to the Stage I gold mineralizing event. Zoned quartz-calcite veins

are interpreted to have formed via multiple opening stages, therefore the calcite margins of these veins

are considered older than the quartz cores. Type 2 veins are commonly, although not always,

surrounded by wide (20-50mm) ankerite alteration zones and clusters of large, inclusion-rich pyrite

grains along the vein selvedges. These pyrite grains typically exhibit a “dirty”, mineral inclusion-rich

core surrounded by a “clean”, inclusion free rim. Mineral inclusions comprise abundant silicates, minor

sulfides (e.g. galena, sphalerite), iron oxides (e.g. magnetite, hematite, ilmenite) and rare gold blebs.

Quartz grains in Type 2 veins have undergone partial dynamic recrystallization by grain boundary

migration and sub-grain rotation. Grain boundaries are often highly irregular and protrude into

neighboring grains, although the degree to which individual samples were recrystallized varies. Sub-

grain development is minor and is predominantly concentrated along the outer vein edge. Relict grains

locally exhibit undulose extinction and lattice-preferred orientation (c.f. Passchier and Trouw, 1996).

Type 3 veins comprise quartz, (Fig. 4c) with or without minor calcite and sericite. The veins are

composed almost entirely of coarse-grained (1-5mm) clear quartz overprinted by accessory calcite and

rare sericite. The veins form breccias within M2 quartz-feldspar porphyries and can be distinguished

from Type 2b veins by their coarse grain size, minor calcite and lack of an alteration selvedge. Quartz

grains within these veins show evidence that they have undergone partial dynamic recrystallization by

grain boundary migration. This evidence includes diffuse and highly irregular grain boundaries.

Type 4 veins, which host Fracture-style mineralization, are composed of sericite, chlorite and

pyrite , form thin (20-200µm) stringer veins (Fig. 4d), and only occur in M2 quartz-feldspar porphyries.

Pyrite is located as large subhedral to euhedral grains or as aggregates of fine subhedral to euhedral

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crystals, and commonly contains abundant silicate and sulfide inclusions. Pyrite hosts gold as rounded

inclusions within grains and localized along pyrite grain boundaries.

Fluid Inclusion Analytical Procedures The first author logged seven diamond drill holes within the Hampton-Boulder and Jubilee open

pits and underground workings. The chosen holes were selected because they intersected the hanging

wall, ore zones and footwall at depths from the present surface to 250m below the pit floor, they all

contained high-grade (>3.0 g/t Au) ore zones and more than one mineralization style was represented in

each hole. Approximately 70 samples representing the different mineralization styles and stages were

collected for further analysis. Of these, 18 quartz and calcite vein samples were prepared as 80µm

double-polished thick sections and then petrographically examined for quartz textures and fluid

inclusions. Six samples representing type 1 (one), type 2 (two), type 3 (two) and quartz-carbonate

alteration associated with contact style mineralization contained fluid inclusions large enough (>5µm)

to conduct detailed microthermometric and laser Raman analyses. These samples were examined

petrographically prior to microthermometric analysis in order to determine the types of inclusions

present in the samples, to describe their morphology, distribution, relative timing, and identify fluid

inclusion assemblages (c.f Goldstein and Reynolds, 1994) in order to assess whether inclusions had

undergone post-entrapment modification or were the result of fluid immiscibility. Over 500 fluid

inclusion measurements were collected in quartz from Type 2 quartz-calcite veins and Type 3 quartz

veins, and from quartz alteration associated with Stage II gold mineralization. Type 1 boudinaged veins

contained only rare inclusions suitable for analysis due to the almost complete dynamic

recrystallization of the quartz. Suitable inclusions in calcite (Type 2 quartz-calcite veins) did not appear

to have undergone any post-entrapment modifications, therefore were also measured. Fluid inclusions

in all samples typically ranged in size from <1µm to approximately 30µm and varied in morphology

from highly irregular to rounded to negative crystal shaped. Most inclusions selected for

microthermometric analysis ranged between 3µm and 15µm in the longest dimension; unusually large

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or highly irregular inclusions were not analyzed as these inclusions are commonly subject to post-

entrapment modification (Roedder, 1984).

Microthermometric data were collected using a fully automated Linkham THMSG heating and

freezing stage, which has a temperature range of -196° to +600°C. The stage was calibrated against the

melting point of pure CO2 (-56.6) and pure H2O (0.0°C), and the critical point of pure H2O (374.1°C)

using SynFlinc synthetic fluid inclusion standards. Accuracy of the stage during low-temperature

(<32°C) measurements was between ± 0.1° and ±0.4°C and during high temperature measurements

(>100°C) was ±4.0°C, whereas precision was to 0.1°C at all temperatures. In order to observe low

temperature phase transitions in all inclusion types, inclusions were first super-cooled to around -70°C

for aqueous inclusions, -110°C for aqueous-carbonic inclusions, and -196°C for methane inclusions,

then reheated slowly at 1°/minute near expected phase transitions. During heating experiments, fluid

inclusion chips were heated at 5°C/minute below 200°C and 1°C/minute above 200°C; measurements

were obtained firstly from liquid-rich then vapor-rich inclusions in order to avoid destroying vapor-rich

inclusions prior to obtaining homogenization temperatures.

The cycling technique of Goldstein and Reynolds (Goldstein and Reynolds, 1994) was

employed during heating and freezing experiments in order to obtain accurate phase transition

temperatures. Salinity (equiv. wt% NaCl), bulk composition and density were calculated using

MacFlinCor (Brown and Hagemann, 1995) and the equations of state for H2O-NaCl-KCl (Bodnar and

Vityk, 1994), and H2O-CO2-CH4-NaCl and CO2-CH4 (Jacobs and Kerrick, 1981). The graphical

methods of Swanenberg (1979) and Thiery et al. (1994) were used to estimate the molar proportions of

CO2 and CH4. The relative proportions of CO2 and CH4 are reported in mole percent (%) and density is

reported in grams per cubic centimeter (g/cm3).

Laser Raman spectroscopy was used to quantify the content of the gas phases in fluid

inclusions, and to identify the nature of the daughter crystals. Laser Raman spectra were recorded at

Geoscience Australia on a Dilor® SuperLabram spectrometer equipped with a holographic notch filter,

600 and 1800 g/mm gratings, and a liquid N2 cooled, 2000 x 450 pixel CCD detector. The inclusions

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and daughter crystals were illuminated with 514.5 nm laser excitation from a Melles Griot 543 argon

ion laser, using 5 mW power at the samples, and a single 30 second accumulation. A 100X Olympus

microscope objective was used to focus the laser beam and collect the scattered light. The focused laser

spot on the samples was approximately 1 μm in diameter. Wave numbers are accurate to ± 1 cm-1 as

determined by plasma and neon emission lines. For the analysis of CO2, O2, N2, H2S and CH4 in the

vapor phase, spectra were recorded from 1000 to 3800 cm-1 using a single 20-second integration time

per spectrum. The detection limits are dependent upon the instrumental sensitivity, the partial pressure

of each gas, and the optical quality of each fluid inclusion. Raman detection limits (Wopenka and

Pasteris, 1987) are estimated to be around 0.1 mole percent for CO2, O2 and N2, and 0.03 mole percent

for H2S and CH4. Errors in the calculated gas ratios are generally less than 1 mole percent.

Fluid Inclusion Study

Location, composition and petrography of fluid inclusions

Fluid inclusions are abundant in quartz and calcite and occur as clusters within single grains and

along healed fractures both entirely within and cross-cutting grain boundaries. Detailed petrography

revealed four compositional fluid inclusion types: (I) CH4, (II) H2O-CO2, (III) CO2-rich, and (IV) H2O-

rich. (Fig. 5).

Type I CH4 inclusions are dark, generally rounded, and are always monophase at room

temperature. These inclusions are subdivided further based on their mode of occurrence. Type Ia

inclusions (Fig. 5a) are located within clusters as small (~10µm), negative crystal shaped primary

inclusions, and are restricted to the calcite selvedge of Type 2a zoned quartz-carbonate veins. Type Ib

(Fig. 5b) inclusions occur as secondary trails of large (10-30µm) irregular inclusions, elongate in the

trail orientation, in both Type 2 and 3 veins. Laser Raman analysis confirmed these as

CH4±C2H6±C3H8.inclusions.

Type II H2O-CO2 (Fig. 5c, 5d) inclusions are two- or three-phase at room temperature, and are

the most common inclusion in Types 2 and 3 veins, and in quartz and calcite alteration. They are

typically small, ranging in size from 5-15µm, and are usually sub-rounded, except when they are

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trapped in calcite, where they are negative-crystal shaped. Type II inclusions are situated in primary

clusters or pseudo-secondary trails and typically display constant phase ratios of 0.3 to 0.4 in a single

trail or cluster within Type 2 veins, but have varied phase ratios, from 0.2 to 0.9 within a single trail or

cluster in Type 3 veins. In both vein types approximately 30% of inclusions contain tiny (<1µm)

rounded, cubic or triangular opaque daughter crystals (Fig. 5c) of unknown compositions and rarely

(<5% of inclusions) may contain larger (up to 5µm) ovoid or rod-shaped transparent nahcolite

(NaHCO3, determined by laser Raman analysis) daughter crystals (Fig. 5d).

Type III CO2±CH4 inclusions (Fig. 5e) are one phase at room temperature and within a single

trail or cluster display constant phase ratios around 0.9. They are ovoid to sub rounded, typically occur

in primary clusters or secondary trails, and range in size from 5-10µm. Up to 20 percent of invisible

H2O may form a thin film along inclusion walls (Roedder, 1972).

Type IV H2O-rich aqueous inclusions (Fig. 5f) are two phase at room temperature. Some

inclusions in Type 3 veins contain small amounts (less than 2.2 molal, (Ellis and Golding, 1963;

Roedder, 1984; Hedenquist and Henley, 1985) dissolved CO2, evidenced by the formation of clathrate

during freezing experiments and a double jerk of the bubble during freezing cycles despite the absence

of a separate liquid carbonic phase at temperatures below the CO2 critical point. Distribution and

occurrence of the aqueous inclusions defined two inclusion populations: (1) irregularly shaped

inclusions that occurred rarely in primary clusters or more commonly in pseudosecondary trails, and

which rarely contained opaque daughter minerals, and (2) rounded to ovoid shaped inclusions that

occupy extensive fracture zones and form broad secondary trails. The volume percent vapor of both

populations is typically between 5 and 10 percent. Inclusions of both populations are typically very

small (1-10µm), and are mostly elongate in the direction of the trail.

Relative timing constraints

The earliest measured inclusions are interpreted to be those that are located in the calcite

margins of zoned Type 2 quartz-calcite veins. These comprise Type I CH4 inclusions and Type II H2O-

CO2 inclusions, which occur in discrete primary mono-inclusion clusters. There are no cross-cutting

15

relationships observed between these two fluid inclusion types, therefore it is unclear how they relate to

each other paragenetically.

Aqueous-carbonic and aqueous inclusions in Type 2 veins, which are found in M1 intermediate

porphyries and formed synchronous with D3NC deformation, are interpreted to predate those in Type 3

veins, which cross-cut D3NC foliation. Carbonic inclusions, observed in Type 3 veins only, likely post-

date the aqueous-carbonic inclusions, however there are no direct cross-cutting relationships observed

between these two inclusion populations. Secondary trails of high-salinity H2O-rich inclusions crosscut

the aqueous-carbonic inclusions in both Type 2 and 3 veins, and in quartz and calcite alteration

associated with Stage II Contact-style gold mineralization. Secondary trails of CH4-rich inclusions

cross-cut all other inclusion types.

Microthermometry and laser Raman data and interpretation

Type I CH4 fluid inclusions: Methane inclusions in calcite and quartz did not freeze at the lower

temperature limit of the Linkham stage (-196°C). Primary inclusions in calcite formed a vapor bubble

at low temperatures (-100°C); upon warming these inclusions homogenized to liquid between -76°C

and -73°C. The composition of these inclusions was not confirmed by laser Raman analysis. Secondary

inclusions in Types 2 and 3 quartz veins also formed a vapor bubble at low temperatures, but in

contrast to the primary calcite-hosted inclusions, they homogenized to liquid at around -90°C. Laser

Raman analyses on secondary quartz-hosted inclusions confirmed them as methane-dominant (95-100

mole % CH4) with minor N2 (up to 3 mole %) and trace (1 mole %) C2H6 (ethane) and C3H8 (propane).

These inclusions had densities of 0.26 g/cm3 (Table 2).

Type II H2O-CO2 fluid inclusions: Aqueous-carbonic inclusions in calcite from Type 2 veins are

located in primary clusters. Inclusions either homogenized to liquid (ThTOT (L)) at 270°C ± 1.0°C or

decrepitated via expansion of the vapor phase (ThCREP (V)) at 267°C ± 0.4°C. Melting of the carbonic

phase (TmCO2) ranged between -56.8°C and -56.6°C (Fig. 6) indicating that the gas phase comprised

nearly pure CO2. Clathrate melting temperatures (TmCLATH) ranged between 7.6 and 9.3°C (Fig. 7),

giving calculated salinities between 1.4 and 4.6 weight percent NaCl equivalent. The CO2 phase

16

homogenized to liquid between 28.9 and 30.8°C (Fig. 6). Inclusions contained between 8 and 27 mole

percent CO2 and had calculated bulk densities ranging between 0.73 and 0.86 g/cm3 (Table 2).

In both Types 2 and 3 veins most of the aqueous-carbonic inclusions in quartz decrepitated

before final homogenization. Where observed, homogenization to the liquid phase occurred between

330°C and 350°C (mean 337°C ± 15°C) in Type 2 veins and between 180°C and 365°C, (mean 295°C

± 44°C) in Type 3 veins. Melting of the carbonic phase (TmCO2) in inclusions from Type 2 veins

occurred at slightly lower temperatures (-62.0 to -56.6°C) than in inclusions from quartz-calcite

alteration and Type 3 veins (-58.1 to -56.6°C) (Fig. 6), which indicates they contained higher

concentrations of other gases, for example methane. Laser Raman analysis, which identified up to 39

mole% CH4 in aqueous-carbonic inclusions from Type 2 veins, confirmed this (Table 2).

Homogenization of the carbonic phase to liquid occurred from 6.5° to 25.8°C in inclusions from Type

2 veins and 11.8° to 30.8°C in inclusions from quartz-calcite alteration and Type 3 veins (Fig. 6, Table

2). Fluid densities, calculated using the graphical methods of Swanenberg (1979) ranged between 0.6

and 1.0g/cm3, although inclusions in Type 3 veins had a narrower range (Table 2). Final clathrate

melting temperatures ranged between 5.8° and 9.8°C (Fig. 7) in inclusions from both vein types and

quartz-calcite alteration, equating to average salinities between 0.4 and 7.4 weight percent NaCl

equivalent, calculated using MacFlinCor (Brown and Hagemann, 1995) and the equations of state for

H2O-NaCl-KCl (Bodnar and Vityk, 1994), and H2O-CO2-CH4-NaCl (Jacobs and Kerrick, 1981).

Type III CO2-rich fluid inclusions: Melting temperature of the carbonic phase in CO2-rich

inclusions from Type 3 veins ranged from -57.3°C to -56.6°C (Fig. 6) indicating that the inclusions

were essentially almost pure CO2, with less than 0.05 mole % of other gases. The ThCO2 ranged from

6.2°C to 30.8°C (Fig. 6), although 51 percent of the inclusions clustered between 15°C and 24°C.

Calculated densities of the carbonic phase varied from 0.5 to 0.9 g/cm3 with less than 3 mole percent

CH4 (Table 2).

Type IV H2O-rich fluid inclusions: Aqueous inclusions containing trace dissolved CO2 in

quartz-calcite alteration and Type 3 veins displayed eutectic temperatures (TE) between -20 and -24°C

17

indicating that the fluids were H2O-NaCl dominated (Borisenko, 1977; Crawford, 1981). All but three

inclusions homogenized to liquid between 140°C and 267°C. The remaining inclusions decrepitated to

liquid at 229°C and 236°C or via expansion of the vapor phase at 252°C. The TmICE ranged between -

6.1 and -0.5°C (Fig. 7). The presence of CO2 affects the salinity measurements, as low levels of CO2

will depress the ice melting temperature by up to 1.5°C (Hedenquist and Henley, 1985), however,

clathrate melting temperatures in the absence of liquid CO2 invalidate salinity calculations using

TmCLATH (Diamond, 1992). Calculated apparent salinities (maximum salinity) of Type IIb inclusions

ranged between 0.8°C and 9.3 equivalent weight percent NaCl and densities ranged between 0.8 and

1.0 g/cm3 (Table 2).

Aqueous inclusions without dissolved CO2 also had eutectic temperatures around -20°C,

indicating that these fluids were also within the H2O-NaCl system. Inclusions in Type 2 quartz veins

homogenized to liquid between 173° and 351°C (Fig. 6). The TmICE ranged between -9.9°C and -0.3°C

(Fig. 7) correlating to calculated salinities between 0.8 and 13.8 weight percent NaCl equivalent and

densities between 0.76 and 1.04 g/cm3. In Type 3 quartz veins, final homogenization occurred at much

lower temperatures, between 90° and 152°C (Fig. 6). Ice melting temperatures ranged between -7.0°

and -0.2°C (Fig. 7) correlating to calculated salinities between 0.3 and 10.5 weight percent NaCl

equivalent and densities of 1.0 g/cm3 (Table 2).

Secondary H2O-rich inclusions in both Types 2 and 3 veins had eutectic temperatures around -

55°C placing them in the H2O-NaCl-CaCl2 system (Borisenko, 1977; Crawford, 1981). Total

homogenization to liquid for all inclusions took place between 55°C and 118°C. The TmICE ranged

between -22.9°C and -15.2°C (Fig. 7). Calculated salinity ranged between 18.4 and 23.2 equivalent

weight percent NaCl and density between 1.09 and 1.17 g/cm3 (Table 2).

Trapping Conditions Given the broad two-phase field in the H2O-CO2-NaCl system (Takenouchi and Kennedy,

1965; Gehrig et al., 1980), it is important to determine whether the mixed H2O-CO2 inclusions

observed at New Celebration could have resulted from phase immiscibility processes. Mixed aqueous-

18

carbonic inclusions in calcite and quartz from Type 2 veins did not display liquid- and vapor-rich end

members within individual trails or clusters, and exhibited only minor variation in bulk composition or

molar volumes, thereby ruling them out as the product of phase separation (c.f. Ramboz et al., 1982). In

contrast, aqueous-carbonic inclusions from Stage II-related Type 3 quartz veins and quartz-calcite

alteration did display partial evidence for fluid immiscibility including: (a) liquid-rich and vapor-rich

end members in some primary clusters or pseudosecondary trails (Fig. 8), (b) total homogenization into

liquid and vapor at the same temperature of at least some of the inclusions, and (c) variable bulk

compositions and molar volumes within an individual trail or cluster.

The lack of conclusive evidence for fluid immiscibility associated with H2O-CO2 inclusions in

Type 2 quartz veins means that independent pressure and temperature estimates must be applied to

determine the trapping conditions of these fluids (c.f. Roedder, 1984), as homogenization temperatures

represent minimum trapping temperatures. Phengite geobarometry on gold-related alteration zones of

the Southern Ore Zone constrains formation pressures to between 3.2 and 4.2 kilobars (Williams,

1994). Regional greenschist facies metamorphism, interpreted to be broadly contemporaneous with

orogenic gold mineralization in the Kalgoorlie-Norseman corridor (McNaughton et al., 1990; Witt,

1991), constrains formation conditions to between 300 and 500°C and a minimum of 2 kilobars (c.f.

Spear, 1995).

Figure 9 illustrates isochores calculated using MacFlinCor (Brown and Hagemann, 1995) from

the different fluid inclusion types at New Celebration. Using the isochores in Figure 9 and the

independent geothermobarometric constraints outlined above, an approximate P-T-t path for the

hydrothermal fluids circulating through the Boulder-Lefroy fault segment is displayed in Figure 10.

The earliest observed aqueous-carbonic inclusions in calcite and by inference, the early primary

methane inclusions formed between 270° and 500°C at 1 to 3 kilobars. Aqueous-carbonic inclusions in

Type 2 veins constrains Stage I gold mineralization to between 300° and 500°C and 2.5 to 4.2 kilobars,

which corresponds to crustal depths between 10 and 15 kilometers below the surface. The intersection

between the isochores and the solvus for aqueous-carbonic inclusions in Type 3 veins constrain Stage

19

II gold mineralization to temperatures between 280° and 360°C and pressures between 1 and 3.5

kilobars, corresponding to crustal depths between 4 and 10 kilometers. Carbonic inclusions, interpreted

as trapped during the final phases of Stage II gold mineralization, have estimated trapping temperatures

between 280° and 360°C and trapping pressures between 0.8 and 1.6 kilobars. Pressure corrected (c.f.

Potter, 1977) low salinity secondary aqueous inclusions are trapped at about 260°C and a maximum of

3.5 kilobars. Maximum trapping temperatures and pressures for high salinity secondary aqueous

inclusions and methane inclusions, observed in all vein types in addition to quartz and calcite

alteration, formed at temperatures around 100-180°C and pressures estimated to range from 0.4 to 1.0

kilobars.

In situ Fluid Inclusion Laser-Ablation ICP-MS Methodology Selected single H2O-CO2 and H2O-rich fluid inclusions from Types 2 and 3 veins and quartz

alteration were analyzed at the University of Leeds using an ArF 193nm Geolas Q Plus excimer laser

equipped with imaging optics (Gunther et al., 1997; Gunther et al., 1998). The entire contents of the

inclusion (liquid, vapor and solid daughter crystals where trapped) were transported to the plasma as an

aerosol using He carrier gas, then the samples were analyzed with an Agilent 7500c quadrupole ICP-

MS equipped with an octopole reaction cell. Fluid inclusion analyses were calibrated using NIST SRM

610 and 612, an in-house EMPA glass standard and capillaries filled with standard solutions. Signal

data were processed using a graphical user-interfaced software package developed at the University of

Leeds (Allan et al., 2005). In order to ensure that the results represented the fluid inclusion contents and

not host vein mineral concentrations, only spectra with coincident Na and other cation peaks were

processed. Inclusion-free quartz was check analyzed for interference and produced no signal. The

absolute element concentrations of fluids in individual fluid inclusions were determined by charge

balancing against the H2O-NaCl equivalent chloride molality of each fluid inclusion population, as

determined by microthermometric heating/freezing experiments prior to the laser ICP-MS analysis. For

a detailed description of the laser ICP-MS analytical process refer to Allan et al. (2005).

20

In situ Fluid Inclusion Laser-Ablation ICP-MS Results Gold at concentrations up to 51ppm were recorded in aqueous-carbonic fluid inclusions

associated with gold mineralization. Analyses also revealed that gold-related fluid inclusions contained

significant concentrations of other metals such as Cu, Pb and Zn (Table 3).

Type 2 veins – Stage I gold-related fluids

The H2O-CO2 inclusions in Type 2 veins are Na-Ca dominant, with subordinate K and Mg.

Individual fluid inclusions contained up to 51ppm gold although average concentrations were around

5ppm (n=80). Concentrations of other metals were generally low, although these inclusions did contain

up to 163ppm Cu, 75ppm Zn and 43ppm As.

Type 3 veins and quartz alteration – Stage II gold-related fluids

The H2O-CO2 inclusions in Type 3 veins and quartz alteration associated with Contact style

mineralization contained higher Na, Mg and K concentrations, but lower Ca than those in Type 2 veins.

Stage II fluids had up to 33ppm Au, and generally contained higher concentrations of Cu, Pb, Zn, Sr,

As, Sb, Bi, Sn, Mn and Fe than fluids associated with Stage I gold mineralization. The H2O-rich

inclusions from Type 3 veins were Na-Mg dominant, with lesser K than the mixed inclusions.

The Au values reported from both Types 2 and 3 veins are consistent with the experimental

work of Mikucki and Ridley (1993) and Mikucki (1998), who determined that at temperatures between

300° and 550°C, gold transported as a bisulfide complex (Au(HS)2-) could have solubilities exceeding

10-10,000 ppb Au. They also exceed the minimum 5ppb Au concentration required to form an ore fluid

capable of forming a gold deposit (Heinrich et al., 1989).

Post-gold fluids

High salinity H2O-rich fluids measured in Type 3 veins are Na-K-Ca-dominated (K/Ca and

Na/K ratios of 5.9 and 3.2, respectively), with subordinate Mg (Table 3). They contain elevated Cu, Pb,

Sn, Ba and Mn relative to the H2O-CO2 inclusions, whereas Fe and Zn are lower. Silver and gold occur

at concentrations of up to 85.7 ppm and 1.6 ppm (n=9), respectively.

21

Comparison of New Celebration Metal and Cation signatures with other hydrothermal fluid systems

There are few published data of metal concentrations in hydrothermal fluids from orogenic lode

gold deposits, and the majority of those published present bulk crush-leach analytical techniques.

Diamond (1990) and Yardley (1993) examined the fluid characteristics of metamorphic gold-quartz

veins from Brusson, in NW Italy and Pike (1993) studied low-salinity gas-rich fluids in pegmatites

from the Muiane deposit, Mozambique. More recently Olivo et al. (2006) employed single inclusion

laser ablation-time of flight-inductively coupled plasma-mass spectrometry (LA-TOF-ICPMS), in

conjunction with crush-leach and microthermometry, to evaluate the fluid compositions in barren and

gold-bearing veins from the Sigma deposit in Canada. None of these studies presented gold data.

Relative to aqueous-carbonic fluids from Muiane or Brusson, K, Mg, Cu, Mn and Fe concentrations in

gold-related aqueous carbonic fluid inclusions at New Celebration are elevated, whereas Na

concentrations are lower. Minor element/Na ratios of New Celebration fluids are generally an order of

magnitude lower than those from the Sigma deposit, with the exception of As, which is higher at New

Celebration. Major element/Na ratios (Mg, K, Ca), however, are up to an order of magnitude higher in

the New Celebration fluids.

More single inclusion data are available from porphyry systems, generally because the fluid

salinities are higher, although there is still a significant dearth of in situ Au analyses. Fluids from the

Butte porphyry system (Rusk et al., 2004), contain Na, K, Pb, Zn and Mn in similar concentrations to

gold-related fluids from New Celebration. Ulrich et al. (1999) publish Au concentrations averaging up

to 10 ppm in vapor inclusions from the Grasberg porphyry Cu-Mo-Au deposit, however, these Au

concentrations were analyzed from high-salinity inclusions. Something about intrusion related gold

systems in here.

The post-gold hydrothermal fluids at New Celebration are low temperature, high salinity fluids

with a characteristic Na, K and Mg signature. When comparing these fluids with data sets from

Canadian shield brines, sedimentary basin fluids, metamorphic fluids, and geothermal fluids (Yardley,

2005 and references therein), it is evident that the shield brines and basin fluids show no similarities to

22

the New Celebration post-gold fluids. The metamorphic, geothermal and magmatic fluids, however,

exhibit a number of similarities; Na, K and Mg concentrations are comparable in all fluid types,

whereas Ca and Cu concentrations in the New Celebration fluids are most similar to magmatic fluids.

Lead and Zn concentrations are more closely aligned with metamorphic or geothermal fluids.

Sulfur Isotope Geochemistry The δ34S isotopic composition of pyrite from fifteen samples representing Stage I and Stage II

gold mineralizing events and four mineralization styles were analyzed by either Nd-YAG laser ablation

of in situ sulfides (Huston et al., 1995) or conventional techniques for pyrite separates (Robinson and

Kusakabe, 1975) at the Central Science Laboratory (CSL), at the University of Tasmania. Thirty in situ

analyses and nine conventional analyses were collected for this study. The conventional analyses

represented an initial reconnaissance study to evaluate the potential for a detailed in situ analysis of

ore-related sulfide. All results are reported in parts per thousand (‰) relative to the Canyon Diablo

Troilite (CDT).

The majority of both Stage I and II gold-related pyrites at New Celebration had negative δ34S

values, (Table 4, Fig. 11) although the range of values both within and between mineralization styles

varied widely. Stage I gold related samples ranged from -7.6 per mil to +3.8 per mil (mean -2.6‰)

whereas Stage II gold related samples ranged from -10.6 per mil to -3.2 per mil (mean -7.1‰).

These values contrast with the predominantly positive δ34S values (0-5‰) reported by Golding

et al. (1990) and Hodkiewicz (2003 and references therein), for ore-related pyrites from most gold

deposits in the Eastern Goldfields (with the exception of Porphyry, the Golden Mile, and Victory-

Defiance) and 0-9 per mil for ore-related sulfides in Archean orogenic lode gold deposits worldwide

(with the exception of Hemlo, Lakeshore/Macassa, Canadian Arrow, and Kelore, which have much

larger δ34S ranges) reported by Colvine et al. (1988) and McCuaig and Kerrich (1998), but are

consistent with previous analyses of ore-stage pyrite from New Celebration undertaken by Hodkiewicz

(2003). Clearly, the fluids that formed the New Celebration deposits were significantly more oxidized

than the average Archean lode gold deposit (c.f. McCuaig and Kerrich, 1998). Either they were

23

intrinsically oxidized from source or they were oxidized during gold precipitation; by in-situ fluid

oxidation due to reaction with iron-rich wall rocks (Couture and Pilote, 1993), by fluid mixing

(Uemoto et al., 2002) or by fluid oxidation during phase separation (Drummond and Ohmoto, 1985).

Fluid Redox and Ore Precipitation Gold mineralization occurs in response to changing chemical conditions of the ore fluid,

typically the fluid redox state or pH, which takes place due to physical changes to the ore fluid, such as

fluid immiscibility, fluid mixing or interaction with reactive wall rocks (Seward, 1973, 1984; Mikucki

and Groves, 1990; Mikucki, 1998). According to Lambert et al., (1984), Phillips et al., (1986) and

Golding et al., (1990) an increase in the redox state of the fluid lowers gold solubility significantly,

thereby creating conditions that favor gold precipitation.

Interaction between the ore fluids and iron-rich wall rocks likely facilitated much of the gold

mineralization at New Celebration. In all mineralization styles pyrite hosts gold, and gold enrichment

shows a close correlation with increasing pyrite (Williams, 1994; Nichols, 2003). Additionally, gold is

located predominantly within the iron-rich wall rock in all mineralization styles except Fracture-style,

where narrow sericite-filled cracks contain the gold-bearing pyrite. Extensive ankerite alteration

accompanies all gold mineralization styles, and pyrite replaces magnetite with increasing proximity to

mineralization. The unaltered intermediate and felsic porphyry host rocks likely did not provide enough

iron to facilitate wall rock reactions, however, extensive pre-mineralization magnetite and hematite

alteration (Nichols, 2003; Nichols et al., submitted) resulted in a significant increase in the amount of

modal iron. The correlation between pyrite abundance and gold enrichment (Nichols et al., in revision)

suggests that sulfidation of iron-rich wall rocks was the mechanism by which the majority of gold

precipitated at New Celebration. Palin and Xu (2000) indicated that this would not effect a change to

the oxidation state of the dissolved sulfur species, therefore there would be no shift to the isotopic

composition of pyrite. This suggests that the sulfur isotopic composition of ore-stage pyrite reflects the

composition of the ore fluids. Sulfur isotope and LA-ICP-MS evidence point to different origins for

Stage I and Stage II ore fluids and suggest a fluid source switch between the two gold mineralizing

24

events from an early likely dominantly metamorphic derived fluid to a later possibly magmatic fluid,

coinciding with the emplacement of the M2 felsic porphyries and their inferred underlying magma

chambers. This is consistent with the recent findings of Mueller (2007) who considers that the giant

Golden Mile deposit, located to the north of New Celebration along strike of the BLFZ formed due to

oxidized magmatic fluids ascending from buried subduction-related monzodiorite-tonalite plutons.

An alternative is that gold mineralization took place due to in situ fluid oxidation, either by wall

rock reaction or fluid immiscibility. Hodkiewicz (2003) determined a broad negative correlation (r2-

0.73, n=5) between gold grade and sulfide sulfur isotopic composition at New Celebration and

interpreted this as evidence for in situ ore fluid oxidation and gold precipitation by carbonate alteration

of host rock magnetite. In contrast, this study found no correlation between sulfide sulfur isotopic

composition and gold grade (r2=0.10, n=28). Further, magnetite carbonation is a poor mechanism for

oxidizing ore fluids as typical lode-gold ore fluids contain high concentrations of CO2 and CH4, which

provides substantial buffering capacity, and only leads to ore fluid oxidation at very low fluid/rock

ratios (E.J. Mikucki unpub. report, 2001). This is not compatible with the significant hydrothermal

fluid flow and high fluid/rock ratios expected within a crustal scale fault system such as the BLFZ and,

therefore can be discounted as a mechanism to precipitate gold or oxidize ore fluids at New

Celebration. Fluid inclusion petrography indicates at least intermittent phase immiscibility during Stage

II gold mineralization. During phase separation reduced gases (H2S, CH4 and H2) are preferentially

partitioned into the gas phase (Drummond and Ohmoto, 1985), thus the liquid becomes more oxidizing.

As a result, some of the remaining reduced species in the liquid, such as H2S, will be oxidized to HSO4-

which is enriched in 34S. Consequently, the reduced sulfur left behind is depleted in 34S therefore

sulfides that precipitate from the residual liquid phase are also 34S depleted. Phase separation is

consistent with the observations made from Type 3 quartz veins and quartz and carbonate alteration

related to Stage II gold mineralization and accounts for both the negative sulfur isotopic composition

and the spread in δ34S ratios observed in Stage II ore-related pyrites.

At least two ore-forming processes acting either contemporaneously or sequentially have

25

potentially influenced gold precipitation during the two gold mineralizing stages at New Celebration.

Fluid-wall rock reaction appears to be the dominant process by which gold precipitated, although it did

not cause fluid oxidation, and phase immiscibility is locally important, at least during Stage II

mineralization.

Discussion

Hydrothermal Fluid Model

Detailed fluid inclusion and sulfur isotope analyses of veins associated with pre- syn- and post-

gold mineralization hydrothermal events point towards a complex hydrothermal fluid system within the

western segment of the BLFZ. Combining the structural and hydrothermal chronology outlined in

previous sections, we propose a three-stage model for the development of the New Celebration gold

deposits (Fig.12).

Early Evolution: The formation of the BLFZ occurred subsequent to the emplacement of the

regional volcano-sedimentary sequence, and to regional D1 N-S oriented thrust faulting, during D2NC

ENE-WSW-oriented shortening and crustal thickening (Nichols, 2003; Nichols et al., 2004; Nichols et

al., submitted; Weinberg et al., 2005). The formation of the NNW-trending, sinistral BLFZ during

ESE-WNW-directed shortening (Nichols, 2003; Nichols et al., 2004; Nichols et al., submitted), and (2)

the emplacement of the M1 intermediate plagioclase-phyric porphyritic dike into the fault zone

characterized the onset of D3NC and peak metamorphism. Type 2 quartz-calcite veins emplaced during

the early formation of the BLFZ trapped methane and aqueous-carbonic fluid inclusions in the calcite

margin between 270°C and 500°C and pressures between 1.1 and 3.1 kilobars (Fig. 10).

Syn-gold evolution: Stage I mineralization took place after peak metamorphism during (early)

D3NC deformation (Witt, 1993; Copeland, 1998; Nichols, 2003). Gold precipitated at approximately 10

to 15 kilometers below the surface in a ductile structural regime predominantly by sulfidation of wall

rock magnetite. Characteristically these fluids were Na-dominant, with lesser Ca, K and Mg (K/Ca <1),

and contained ppm level Au, Fe, Cu, Zn and As. Stage II mineralization occurred post-D3NC (Nichols,

2003) during brittle reactivation of the BLFZ at the end of D3NC and during early D4NC (Nichols et al.,

26

submitted). Mineralization took place at shallower levels than Stage I, between approximately 4 and 10

km, likely due to a combination of wall rock sulfidation and phase immiscibility. The hydrothermal

fluids were Na dominant, with lesser Mg, K and Ca (K/Ca >1) in addition to ppm level Au, Fe, Cu, Pb,

Zn, and As. The change in fluid characteristics from Stage I to Stage II suggest a switch in fluid source,

possibly from a metamorphic origin to a magmatic origin, coinciding with the emplacement of the M2

porphyries, although this remains equivocal at present.

Post-gold evolution: Secondary post-gold fluid inclusions in Types 2 and 3 quartz veins record

at least three distinct phases of fault zone reactivation at New Celebration. Low-salinity aqueous fluids

were followed by the infiltration of highly saline aqueous fluids which themselves were followed by

methane fluids. Pressure and temperature trapping estimates for the high salinity and methane fluids are

significantly lower than for all previous fluid inclusion assemblages, suggesting significant uplift and

erosion during the final reactivation stages of the BLFZ.

In summary, the paleohydrothermal evolution of the BLFZ and New Celebration gold deposits

is characterized by discrete pulses of gold-bearing and barren hydrothermal fluids infiltrating the fault

as a consequence of distinct deformation events (D3NC to D4+NC) including several reactivation events.

At least two gas-rich fluid events are recorded that cannot be linked to gold mineralization. The gold

mineralization stages are characterized by aqueous-carbonic inclusions and as such are similar to many

other gold-bearing fluids observed in many orogenic gold deposits worldwide. Cation ratios indicate a

fluid source switch between Stage I and Stage II fluids. There is no fluid inclusion evidence for

significant surface water infiltration into the BLFZ at New Celebration (c.f. Hagemann et al., 1993),

therefore, the switch in K/Ca ratios may relate to a change in deep fluid sources such as magmatic or

metamorphic fluids or a combination of the two.

Key factors in the location of the New Celebration deposits

In contrast to most other first order crustal scale fault systems around the world, the BLFZ is

unique in that it hosts the world class New Celebration gold deposits directly within the fault and not

within adjacent higher-order splays. The key factors in the location of the New Celebration deposits

27

within the BLFZ appear to be: (1) the long-lived and complex deformation history of the fault, (2) its

exposure to a number of different fluids, and (3) lithological complexity, which provided appropriate

chemical (Stage I and II) and rheological (Stage II) conditions conducive to gold mineralization.

The fluid inclusion record at New Celebration indicates that fluid flow through the BLFZ

continued over an extended length of time during a number of deformation events and included several

chemically different fluids of potentially diverse origins, at least two of which contained gold and other

metals and contributed to gold mineralization at New Celebration. This is in contrast to other first-order

crustal scale shear zones, such as the Cadillac Tectonic Zone (CTZ) in the Abitibi greenstone belt of

Canada. The CTZ, which is spatially associated with a number of world-class gold deposits hosted

within second- and third-order splays, contains, where fluid inclusions were analyzed, only CO2-

dominated fluids (Neumayr et al., 2007) and is poorly gold endowed. The BLFZ appears to be the most

critical factor in the location of the New Celebration gold deposits as it tapped a number of different

crustal fluids during its long-lived history and facilitated the movement these fluids into zones that

provided the necessary physical and chemical environment for significant gold mineralization.

The presence of iron-rich mafic host rocks and the pre-mineralization hydrothermal magnetite

alteration of otherwise chemically unfavorable iron-poor intermediate host rocks (c.f. Groves, 1990;

Hodgson, 1993) significantly enhanced the potential for the BLFZ to host gold mineralization at New

Celebration. Dilation of the shear zone and an anti-clockwise change in the orientation of the shear

zone away from the average trend of the BLFZ (Hodkiewicz, 2003) during late D3NC and early D4NC

provided space for the emplacement of the M2 porphyry into the fault. This provided a favorable host

for Stage II mineralization during brittle reactivation of the fault, associated failure-induced pressure

reduction and consequent phase separation. Intrusion of the M2 porphyry may also have coincided with

an influx of a second gold-bearing fluid, possibly of magmatic origin, into the shear zone.

Fluid and metal source

As with many orogenic lode gold deposits around the world, the source of the hydrothermal

fluids and metals at New Celebration remain unconstrained. Potassium, Mg and Ca over Na ratios, and

28

high base metal concentrations in Stage II related fluids relative to Stage I indicate that at least two

different gold-bearing fluids were responsible for gold mineralization at New Celebration at different

times. The origins of these fluids are likely metamorphic, or magmatic (Ridley and Diamond, 2000), or

a combination of the two, and maybe locally or regionally derived, however their exact sources are

equivocal.

The relatively high concentrations of the base metals Cu, Pb and Zn in the ore fluids (Table 3),

and the lack of base metal sulfides in the New Celebration gold deposits require an explanation.

Significant amounts of base metals do not typically characterize orogenic lode gold deposits, and the

geochemistry of base metal-bisulfide complexes is poorly understood (Wood and Samson, 1998);

however, recent advances in single-inclusion laser-ablation inductively coupled plasma mass

spectrometry have allowed detailed investigations of ore fluid compositions. Olivo et al (2006) reported

Cu/Na, Pb/Na and Zn/Na ratios up to an order of magnitude higher than those reported in this study,

without any associated base metal mineralization. This would suggest that base metals in lode gold

fluids maybe more common than previously anticipated, but that physico-chemical conditions for the

precipitation of base metals is not favourable. Either the base metal sulfides precipitated at higher or

lower crustal levels in the system than the gold, and were eroded away or not yet exposed or they did

not precipitate at all and instead reached the paleo-surface in the outflow zone of the hydrothermal

system. Further single inclusion analyses of lode gold hydrothermal fluids from other deposits may

indicate whether base metals are a characteristic of orogenic lode gold deposits, or whether they are

unique to New Celebration only.

Timing of mineralization

The absolute timing of gold deposition at New Celebration, and the time gap between the two

mineralizing stages is also unconstrained. Pressure-temperature estimates indicate that Stage II

mineralization occurred after a significant period of interpreted uplift and erosion and during a change

from a ductile to a brittle deformational regime during crustal cooling or increasing strain rate

29

(Weinberg et al., 2005). Whether gold precipitated during two discrete pulses or during continuous

tectonic and fluid evolution of the BLFZ remains presently unclear.

Conclusions Petrographic, fluid inclusion and isotopic analyses of the pre- and syn-gold related veins and

ore-related host sulfides at New Celebration indicate that two stages of gold mineralization formed

from differing hydrothermal fluids under differing P-T conditions during the evolution of the Boulder-

Lefroy fault zone. Stage I gold mineralization took place due to wall rock reaction with pre-existing

magnetite alteration during a ductile deformation regime from low to moderate salinity aqueous-

carbonic fluids trapped at temperatures between 330 and 500°C and pressures between 2.4 and 4.2kbar.

In contrast, Stage II gold mineralization formed due to fault-triggered phase immiscibility, wall-rock

reaction and possible fluid mixing during a brittle-ductile to brittle deformation from low to moderate

salinity aqueous-carbonic fluids trapped at temperatures between 280°C and 360°C and pressures

between 1.5 and 3.5kbar. Cation ratios and metal concentrations indicate that a switch in fluid source

occurred between Stage I and Stage II mineralization, possibly as a consequence of the evolving fault

system tapping a different fluid reservoir at depth. The source of the hydrothermal ore fluids and metals

remains unconstrained; however, they likely originated from the devolatilization of deep crustal rocks

undergoing regional scale metamorphism, from magmatic bodies, or a combination of the two.

This study conclusively illustrates that a first order crustal-scale shear zone contained gold-

bearing fluids during part of its deformation history. Although the role of crustal scale faults as vectors

towards lode gold mineralization in higher order structures has long been recognized (e.g. Eisenlohr et

al., 1989), crustal scale faults have been largely ignored as primary exploration targets. Gold

mineralization at New Celebration clearly relates to the influx of gold-bearing CO2-rich fluids into the

western segment of the Boulder-Lefroy crustal-scale fault zone, where gold precipitated due to the

reaction of the hydrothermal fluids with magnetite-bearing intermediate and felsic wall rocks and phase

separation. The New Celebration deposits are not typical orogenic lode gold deposits in that they are

hosted within a primary crustal scale structure within predominantly intermediate and felsic intrusive

30

rocks; a geological setting mostly considered unfavorable for exploration. This study illustrates that

first-order fault systems do have the potential to host significant gold mineralization where the physico-

chemical parameters are favorable and should be evaluated when exploring in both brownfields and

greenfields terrains.

Acknowledgements This work forms part of the first authors PhD research, undertaken through the Centre for

Exploration Targeting at the University of Western Australia and under the auspices of the Predictive

Mineral Discovery Cooperative Research Centre. JLH gratefully acknowledges receipt of an Australian

Postgraduate Award and a pmd*CRC supplementary scholarship. We would like to thank Mike

Humphries and Sian Nichols of Harmony Gold Mining Company Ltd (South Kal Mines) for providing

technical and logistical support and Bob Hayden, CEO of the pmd*CRC for permission to publish. We

would also like to thank Rich Goldfarb and an anonymous reviewer for their detailed and constructive

comments, which immensely improved the manuscript.

References Allan, M. M., Yardley, B. W. D., Forbes, L. J., Shmulovich, K. I., Banks, D. A., and Shepherd, T. J.,

2005, Validation of LA-ICP-MS fluid inclusion analysis with synthetic fluid inclusions: American Mineralogist, v. 90, p. 1767-1775.

Bateman, R. J., Hagemann, S. G., McCuaig, T. C., and Swager, C., 2001, Protracted gold mineralisation throughout Archaean orogenesis in the Kalgoorlie camp, Yilgarn Craton, Western Australia: structural, mineralogical and geochemical evolution, in Hagemann, S. G., Neumayr, P., and Witt, W. K., eds., World-class Gold Camps and Deposits in the Eastern Yilgarn Craton, Western Australia, with Special Emphasis on the Eastern Goldfields Province, Record 2001/17, Western Australian Geological Survey, p. 63-98.

Bodnar, R. J., and Vityk, M. O., 1994, Interpretation of microthermometric data for H2O-NaCl inclusions, in De Vivo, B., and Frezzotti, M. L., eds., Fluid Inclusions in Minerals: Methods and Applications, Virginia Polytechnic Institute Press, p. 117-130.

Borisenko, A. S., 1977, Study of the salt composition of solutions in gas-liquid inclusions in minerals by the cryometric method: Soviet Geology and Geophysics, v. 18, p. 11-19.

Boulter, C. A., Fotios, M. G., and Phillips, G. N., 1987, The Golden Mile, Kalgoorlie: A giant gold deposit localized in ductile shear zones by structurally induced infiltration of an auriferous metamorphic fluid: Economic Geology, v. 82, p. 1661-1678.

Brown, P. E., and Hagemann, S. E., 1995, MacFlinCor and its application to fluids in Archean lode-gold deposits: Geochimica et Cosmochimica Acta, v. 59, p. 3943-3952.

Colvine, A. C., Fyon, J. A., Heather, K. B., Marmont, S., Smith, P. M., and Troop, D. G., 1988, Archean Lode Gold Deposits in Ontario, Ontario Geological Survey Miscellaneous Paper 139, p. 136.

Copeland, I. K., 1998, Jubilee gold deposit, Kambalda: Australasian Institute of Mining and Metallurgy Monograph 22, p. 219-224.

31

Couture, J. F., and Pilote, P., 1993, The geology and alteration patterns of a disseminated, shear zone-hosted mesothermal gold deposit: the Francoeur 3 Deposit, Rouyn-Noranda, Quebec: Economic Geology, v. 88, p. 1664-1684.

Crawford, M. L., 1981, Phase equilibria in aqueous fluid inclusions, in Hollister, L. S., and Crawford, M. L., eds., Short Course in Fluid Inclusions: Applications to Petrology, 6, Mineralogical Association of Canada, p. 75-100.

Diamond, L. W., 1990, Fluid inclusion evidence for P-V-T-X evolution of hydrothermal solutions in late alpine gold-quartz veins at Brusson, Val d'ayas, Northwest Italian Alps: American Journal of Science, v. 290, p. 912-958.

Diamond, L. W., 1992, Stability of clathrate hydrate + CO2 liquid + CO2 vapour + aqueous KCl-NaCl solutions: Experimental determination and application to salinity estimates of fluid inclusions: Geochimica et Cosmochimica Acta, v. 56.

Dielemans, P., 2000, Structural controls on gold mineralisation in the Southern Ore Zone of the Hampton-Boulder deposit, New Celebration gold mine, Western Australia: Unpub. MSc. thesis, University of Western Australia, 185 p.

Drummond, S. E., and Ohmoto, H., 1985, Chemical evolution and mineral deposition in boiling hydrothermal systems: Economic Geology, v. 80, p. 126-147.

Eisenlohr, B. N., Groves, D. I., and Partington, G. A., 1989, Crustal scale shear zones and their significance to Archaean gold mineralisation in Western Australia: Mineralium Deposita, v. 24, p. 1-8.

Ellis, A. J., and Golding, R. M., 1963, The solubility of carbon dioxide above 100°C in water and in sodium chloride solutions: American Journal of Science, v. 261, p. 47-60.

Gehrig, M., Lentz, H., and Franck, E. U., 1980, Phase equilibria and pVT of binary and ternary mixtures of water, carbon dioxide and sodium chloride up to 3 kb and 550 degrees C: Mineralogical Society Bulletin, v. 49, p. 6.

Golding, S. D., Groves, D. I., McNaughton, N. J., Mikucki, E., and Sang, J. H., 1990, Sulfur isotope studies, in Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold deposits of the Yilgarn Block, Western Australia: Nature, genesis and exploration guides, University of Western Australia, Geology Department and University Extension, v. 20, p. 259-262.

Goldstein, R. M., and Reynolds, T. J., 1994, Systematics of fluid inclusions in diagenetic minerals: SEPM Short Course 31, Society for Sedimentary Geology, 199 p.

Goleby, B. R., Korsch, R. J., Fomin, T., Owen, A. J., and Bell, B., 2000, The AGCRC's 1999 Yilgarn deep seismic survey, Australian Geological Survey Organisation, 2000/34, p. 52-64.

Groves, D. I., 1990, Excursion no. 3: Eastern Goldfields mineral deposits. 1: Overview of gold mineralization in the Norseman-Wiluna belt, in Ho, S. E., Glover, J. E., and Muhling, J. R., eds., Third international Archaean symposium excursion guidebook, Geology Department and University Extension, University of Western Australia, Publication no. 21, p. 307-317.

Groves, D. I., Barley, M. E., and Ho, S. E., 1990, Nature, genesis and tectonic setting of mesothermal gold mineralisation in the Yilgarn Block, Western Australia: Economic Geology Monograph, v. 6, p. 71-85.

Gunther, D., Audetat, A., Frischknecht, R., and Heinrich, C. A., 1998, Quantitative analysis of major, minor and trace elements in fluid inclusions using laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS): Journal of Analytical Atomic Spectroscopy, v. 13, p. 263-270.

Gunther, D., Frischknecht, R., Heinrich, C. A., and Kahlert, H.-J., 1997, Capabilities of an argon fluoride 193 nm Excimer laser for laser ablation inductively coupled plasma mass spectrometry microanalysis of geological materials: Journal of Analytical Atomic Spectroscopy, v. 12, p. 939-944.

Hagemann, S. G., Groves, D. I., Ridley, J. R., and Vearncombe, J. A., 1993, The Archean lode gold deposits at Wiluna, Western Australia: High-level brittle-style mineralization in a strike-slip regime: Economic Geology, v. 87, p. 1022-1053.

32

Hedenquist, J. W., and Henley, R. W., 1985, The importance of CO2 on freezing point measurements of fluid inclusions: evidence from active geothermal systems and implications for epithermal ore deposition: Economic Geology, v. 80, p. 1379-1406.

Heinrich, C. A., Henley, R. W., and Seward, T. M., 1989, Hydrothermal Systems: Adelaide, Australian Mineral Foundation, 74 p.

Hodgson, C. J., 1993, Mesothermal lode-gold deposits, in Kirkham, R. V., Sinclair, W. D., Thorpe, R. I., and Duke, J. M., eds., Mineral Deposit Modeling, Special Paper 40, Geological Association of Canada, p. 635-678.

Hodkiewicz, P., 2003, The Interplay Between Physical and Chemical Processes in the Formation of World-Class Orogenic Gold Deposits in the Eastern Goldfields Province, Western Australia: Unpub. PhD thesis, University of Western Australia, 198 p.

Huston, D. L., Power, M., Gemmell, J. B., and Large, R. R., 1995, Design, calibration and geological application of the first operational Australian laser ablation sulphur isotope microprobe: Australian Journal of Earth Sciences, v. 42, p. 549-555.

Jacobs, G. K., and Kerrick, D. M., 1981, Methane: An equation of state with application to the ternary system H2O-CO2-CH4: Geochimica et Cosmochimica Acta, v. 45, p. 607-614.

Lambert, I. B., Phillips, G. N., and Groves, D. I., 1984, Sulphur isotope compositions and genesis of Archaean gold mineralization, Australia and Zimbabwe, in Foster, R. P., ed., Gold '82: the Geology, Geochemistry and Genesis of Gold Deposits: Rotterdam, A.A. Balkema, p. 373-387.

Langsford, N., 1989, Stratigraphy of Locations 48 and 50, Kalgoorlie Gold Workshop, p. 6. McCuaig, T. C., and Kerrich, R., 1998, P-T-t-deformation-fluid characteristics of lode gold deposits:

evidence from alteration systematics: Ore Geology Reviews, v. 12, p. 381-453. McNaughton, N. J., Cassidy, K., Groves, D. I., and Perring, C. S., 1990, Timing of mineralization, in

Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold Deposits of the Yilgarn Block Western Australia: Nature, Genesis and Exploration Guides: Perth, Department of Geology and University Extension, University of Western Australia Publication No. 20, p. 221-225.

Mikucki, E., and Groves, D. I., 1990, Nature of ore fluid, and transportational and depositional conditions in sub-amphibolite facies deposits: Mineralogical constraints, in Ho, S. E., Groves, D. I., and Bennett, J., eds., Gold deposits of the Archean Yilgarn block, Western Australia: Nature, genesis and exploration guides: Perth, Geology Department (Key Centre) and University Extension, the University of Western Australia, Publication No. 20, p. 212-220.

Mikucki, E., and Ridley, J., 1993, The hydrothermal fluid of Archaean lode-gold deposits at different metamorphic grades: compositional constraints from ore and wallrock alteration assemblages: Mineralium Deposita, v. 28, p. 469.

Mikucki, E. J., 1998, Hydrothermal transport and depositional processes in Archean lode-gold systems: A review: Ore Geology Reviews, v. 13, p. 307.

Mueller, A. G., 2007, Copper-gold endoskarns and high-Mg monzodiorite-tonalite intrusions at Mt. Shea, Kalgoorlie, Australia: implications for the origins of gold-pyrite-tennantite mineralization in the Golden Mile: Mineralium Deposita, v. 42, p. 737-769.

Mueller, A. G., Harris, L. B., and Lungan, A., 1988, Structural control of greenstone-hosted gold mineralization by transcurrent shearing: A new interpretation of the Kalgoorlie Mining District, Western Australia: Ore Geology Reviews, v. 3, p. 359-387.

Nelson, D. R., 1997, Evolution of the Archaean granite-greenstone terranes of the Eastern Goldfields, Western Australia: SHRIMP U-Pb zircon constraints: Precambrian Research, v. 83, p. 57-81.

Neumayr, P., and Hagemann, S. E., 2002, Hydrothermal fluid evolution within the Cadillac Tectonic Zone, Abitibi Greenstone Belt, Canada: Relationship to auriferous fluids in adjacent second- and third-order shear zones: Economic Geology, v. 97, p. 1203-1225.

Neumayr, P., Hagemann, S. E., Banks, D. A., Yardley, B. W. D., Couture, J. F., Landis, G. P., and Rye, R., 2007, Fluid Chemistry and Evolution of Hydrothermal Fluids in an Archaean Transcrustal Fault Zone Network: the Case of the Cadillac Tectonic Zone, Abitibi Greenstone Belt, Canada: Canadian Journal of Earth Sciences, v. 44, p. 745-773.

33

Neumayr, P., Hagemann, S. G., and Couture, J. F., 2000, Structural setting, textures, and timing of hydrothermal vein systems in the Val d'Or Camp, Abitibi, Canada; implications for the evolution of transcrustal, second- and third-order fault zones and gold mineralization: Canadian journal of earth sciences, v. 37, p. 95.

Nichols, S., 2003, Structural control, hydrothermal alteration and relative timing of gold mineralisation at the New Celebration gold deposits, Kalgoorlie, Western Australia: Unpub. BSc (Hons) thesis, University of Western Australia, 62 p.

Nichols, S. J., Hagemann, S. G., Neumayr, P., and Humphries, M., 2004, Structural control, hydrothermal alteration and relative timing of gold mineralisation at the Archaean New Celebration gold deposits, Kalgoorlie, Western Australia., in McPhie, J., and McGoldrick, P., eds., Dynamic Earth; past, present and future. Abstracts - Geological Society of Australia, p. 105.

Norris, N. D., 1990, New Celebration gold deposits, in Hughes, F. E., ed., Geology of the mineral deposits of Australia and Papua New Guinea, Melbourne, Monograph 14, Australasian Institute of Mining and Metallurgy, p. 449-454.

Olivo, G. R., Chang, F., and Kyser, T. K., 2006, Formation of the auriferous and barren North Dipper veins in the Sigma mine, Val d'Or, Canada: Constraints from structural, mineralogical, fluid inclusion and isotopic data: Economic Geology, v. 101, p. 607-631.

Palin, J. M., and Xu, Y., 2000, Gilt by Association? Origins of Pyritic Gold Ores in the Victory Mesothermal Gold Deposit, Western Australia: Economic Geology, v. 95, p. 1627-1634.

Passchier, C. W., 1994, Structural geology across a proposed terrane boundary in the eastern Yilgarn craton, Western Australia: Precambrian Research, v. 68, p. 43-64.

Passchier, C. W., and Trouw, R. A. J., 1996, Microtectonics, Springer. Phillips, G. N., Groves, D. I., Neall, F. B., Donnelly, T. H., and Lambert, I. B., 1986, Anomalous

sulfur isotope composition in the Golden Mile, Kalgoorlie: Economic Geology, v. 81, p. 2008-2015.

Pike, S., 1993, The chemistry of granite derived pegmatite fluids: Unpub. PhD thesis, University of Leeds, 244 p.

Potter, R. W., 1977, Pressure corrections for fluid inclusion homogenization temperatures based on the volumetric properties of the system H2O-NaCl: Journal of Research of the U.S Geological Survey, v. 5, p. 603-607.

Ramboz, C., Pichavant, M., and Weisbrod, A., 1982, Fluid immiscibility in natural processes: Use and misuse of fluid inclusion data II. Interpretation of fluid inclusion data in terms of immiscibility: Chemical Geology, v. 37, p. 29-48.

Ridley, J., and Mengler, F., 2000, Lithological and structural controls on the form and setting of vein stockwork orebodies at the Mount Charlotte gold deposit, Kalgoorlie: Economic Geology, v. 95, p. 85-98.

Ridley, J. R., and Diamond, L. W., 2000, Fluid chemistry of lode gold deposits, and implications for genetic models, in Hagemann, S. G., and Brown, P. E., eds., Gold in 2000, Reviews in Economic Geology, v. 13, p. 141-162.

Robert, F., 1989, Internal structure of the Cadillac tectonic zone southeast of Val d'or, Abitibi greenstone belt, Quebec: Canadian Journal of Earth Sciences, v. 26, p. 2661-2675.

Robert, F., 1990, An overview of gold deposits in the eastern Abitibi subprovince: Canadian Institute of Mining and Metallurgy Special Volume, v. 43, p. 93-105.

Robinson, B. W., and Kusakabe, M., 1975, Quantitative preparation of sulfur dioxide for 34S/32S analyses from sulfides by combustion with cuprous oxide: Analytical Chemistry, v. 47, p. 1179-1181.

Roedder, E., 1972, Compositions of fluid inclusions: US Geological Survey Professional Paper 440-JJ, p. 1-64.

Roedder, E., 1984, Fluid Inclusions, Mineralogical Society of America, 644 p.

34

Rusk, B. G., Reed, M. H., Dilles, J. H., Klemm, L. M., and Heinrich, C. A., 2004, Compositions of magmatic hydrothermal fluids determined by LA-ICP-MS of fluid inclusions from the porphyry copper-molybdenum deposit at Butte, MT: Chemical Geology, v. 210, p. 173-199.

Seward, T. M., 1973, Thio complexes of gold and the transport of gold in hydrothermal ore solutions: Geochimica et Cosmochimica Acta, v. 37, p. 379.

Seward, T. M., 1984, The transport and deposition of gold in hydrothermal systems, in Foster, R. P., ed., Gold '82: The Geology, Geochemistry and Genesis of Gold Deposits: Rotterdam, A.A. Balkema, p. 165-182.

Spear, F. S., 1995, Metamorphic phase equilibria and Pressure-Temperature-Time paths: Washington, Mineralogical Society of America, 799 p.

Swager, C., 1989, Structure of Kalgoorlie greenstones - regional deformation history and implications for the structural setting of the Golden Mile gold deposits, Geological Society of Western Australia Report 25, p. 59-84.

Swager, C., 1997, Tectono-stratigraphy of late Archaean greenstone terranes in the southern Eastern Goldfields, Western Australia: Precambrian Research, v. 83, p. 11-42.

Swager, C., and Griffin, T. J., 1990, Geology of the Archaean Kalgoorlie Terrane (northern and southern sheets), Western Australian Geological Survey, 1:250,000 Geological Map.

Swager, C., and Nelson, D. R., 1997, Extensional emplacement of a high-grade granite gneiss complex into low-grade greenstones, Eastern Goldfields, Yilgarn Craton, Western Australia: Precambrian Research, v. 83, p. 203-219.

Swanenberg, H. E. C., 1979, Phase equilibria in carbonic systems, and their application to freezing studies of fluid inclusions: Contributions to Mineralogy and Petrology, v. 68, p. 303-306.

Takenouchi, S., and Kennedy, G. C., 1965, The solubility of carbon dioxide in NaCl solutions at high temperatures and pressures: American Journal of Science, v. 263, p. 445-454.

Thiery, R., van den Kerkhof, A. M., and Dubessy, J., 1994, vX properties modeling of CH4-CO2 and CO2-N2 fluid inclusions (T<31°C, P<400 bar): European Journal of Mineralogy, v. 6, p. 753-771.

Uemoto, T., Ridley, J., Mikucki, E., Groves, D. I., and Kusakabe, M., 2002, Fluid Chemical Evolution as a Factor in Controlling the Distribution of Gold at the Archean Golden Crown Lode Gold Deposit, Murchison Province, Western Australia: Economic Geology, v. 97, p. 1227-1248.

Ulrich, T., Gunther, D., and Heinrich, C. A., 1999, Gold concentrations of magmatic brines and the metal budget of porphyry copper deposits: Nature, v. 399, p. 676.

Weinberg, R. F., Moresi, L., and van der Borgh, P., 2003, Timing of deformation in the Norseman-Wiluna Belt, Yilgarn Craton, Western Australia: Precambrian Research, v. 120, p. 219-239.

Weinberg, R. F., Van der Borgh, P., Bateman, R. J., and Groves, D. I., 2005, Kinematic History of the Boulder-Lefroy Shear Zone System and Controls on Associated Gold Mineralization, Yilgarn Craton, Western Australia: Economic Geology, v. 100, p. 1407-1426.

Wilkinson, L., Cruden, A. R., and Krogh, T. E., 1999, Timing and kinematics of post-Timiskaming deformation within the Larder Lake-Cadillac deformation zone, southwest Abitibi greenstone belt, Ontario, Canada: Canadian Journal of Earth Sciences, v. 36, p. 627-647.

Williams, H., 1994, The lithological setting and controls on gold mineralization in the Southern Ore Zone of the Hampton-Boulder gold deposit, New Celebration Gold Mine, Western Australia: Unpub. BSc (Hons) thesis, University of Western Australia.

Williams, P. R., and Currie, K. L., 1993, Character and regional implication of the sheared Archaean granite-greenstone contact near Leonora, Western Australia: Precambrian Research, v. 62, p. 343-365.

Witt, W. K., 1991, Regional metamorphic controls on alteration associated with gold mineralization in the Eastern Goldfields province, Western Australia: Implications for the timing and origin of Archean lode-gold deposits: Geology, v. 19, p. 982-985.

35

Witt, W. K., 1993, Gold deposits of the Kalgoorlie-Kambalda-St Ives area, Western Australia: Part 3 of a systematic study of the gold mines of the Menzies-Kambalda region, Geological Survey of Western Australia Record 1992/15, 108 p.

Wood, S. A., and Samson, I. M., 1998, Solubility of ore minerals and complexation of ore metals in hydrothermal solutions, in Richards, J. P., and Larson, P. B., eds., Techniques in hydrothermal ore deposits geology. Reviews in Economic Geology, Volume 10, Society of Economic Geology, p. 33-77.

Wopenka, B., and Pasteris, J. D., 1987, Raman intensities and detection limits of geochemically relevant gas mixtures for a laser Raman microprobe: Analytical Chemistry, v. 59, p. 2165-2170.

Yardley, B. W. D., 2005, Metal concentrations in crustal fluids and their relationship to ore formation: Economic Geology, v. 100, p. 613-632.

Yardley, B. W. D., Banks, D. A., Bottrell, S. H., and Diamond, L. W., 1993, Postmetamorphic gold-quartz veins from N.W. Italy: The composition and origin of the ore fluid: Mineralogical Magazine, v. 57, p. 407-422.

Vein Type

Deformation Event

Timing Mineralogy Structure Alteration Halo

1 D2NC Syn-D2NC Quartz, carbonate Deformed, boudinaged recrystallized veins parallel to D3NC

foliation

Ankerite?

2 D3NC Syn-D3NC Quartz, calcite, pyrite Thin veins, show mutually cross-cutting relationships with D3NC

foliation

Ankerite

3 D4NC Late D3NC or D4NC. Cross-cut D3NC

foliation

Quartz, (carbonate, sericite) Form brittle vein arrays None

4 D4NC Late D3NC or D4NC. Cross-cut D3NC

foliation

Sericite, pyrite Thin veinlets None

Joanna Hodge Table 1

Type I CH4

Type IIH2O-CO2-CH4-NaCl

Type IIICO2-CH4

Type IVH2O

Type 1

Primary & pseudosecondary TmCO2: -56.6ThCO2: 26.8 – 29.0 XCH4: 0 mole%CO2 Density: 0.60 – 0.72 g/cm3

Bulk Density: 0.60 – 0.72 g/cm4

Pseudosecondary H2O-NaCl TmICE: -9.3 - -5.0°CThTOT (L): 122 – 202°CSalinity: 7.8 – 13.2 wt%Bulk Density: 0.94 – 1.00 g/cm3

Calcite

Primary ThTOT (L): -76.4 – -73.0°C

Primary TmCO2: -56.8 – -56.7°CThCO2: 28.9 –- 30.8°CTmCLATH: 7.6 - 9.3°CThDECREP (V): 267.0 – 267.7°CThTOT (L): 268.5 – 270.7°CSalinity: 1.42 – 4.62 wt%XCO2: 8 – 27 mole%XCH4: 0 mole%CO2 Density: 0.40 – 0.60 g/cm3


Quartz

Secondary ThTOT (L): -90.3 – -89.8°C

XCH4: 95-100 mole%XN2: 0-3 mole%XC2H6: 0-1 mole%XC3H8: 0-1 mole%

Primary TmCO2: -61.8 – -56.6°CThCO2: 6.5 –- 25.8°CTmCLATH: 6.0 - 9.8°CThDECREP (V): 226 – 277°CThTOT (L): 328 – 352°CSalinity: 0.42 – 7.38 wt%XCO2: 5 – 73 mole%XCH4: 0 - 39 mole%CO2 Density: 0.49 – 0.87 g/cm3


Solids: opaques, nahcolite

Pseudosecondary H2O-NaClTmICE: -9.9 - -0.5°CThTOT (L): 174 – 272°CSalinity: 0.8 – 13.8 wt%Bulk Density: 0.76 – 0.94 g/cm3

Secondary H2O-NaCl-CaCl2TmICE: -14.8 - -14.7°CThTOT (L): Salinity: 18.4 – 18.5 wt%Bulk Density:

Qz-cc altn

Primary & pseudosecondary TmCO2: -57.8 – -56.6°CThCO2: 11.8 –- 30.8°CTmCLATH: 5.8 - 8.4°C ThDECREP (V): 186 – 364°CThTOT (L-V): 285 – 316°CSalinity: 3.15 – 7.70 wt%XCO2: 10 – 76 mole%XCH4: 0 – 3 mole%CO2 Density: 0.54 – 0.85 g/cm3


Pseudosecondary H2O-NaCl>>CO2

TmICE: -7.0 - -0.2°CThTOT (L): 89 - 117°CSalinity: 0.3 – 10.5 wt%Bulk Density: 0.96 – 0.99 g/cm3

Secondary H2O-NaCl-CaCl2TmICE: -22.9 - -15.4°CThTOT (L): Salinity: 18.7 – 23.2 wt%Bulk Density:

Pseudosecondary H2O-NaCl>>CO2TmICE: -5.8 - -1.1°CThTOT (L): 123 - 152°CSalinity: 1.8 – 8.9 wt%Bulk Density: 0.95 – 0.97 g/cm3

Type 3

Primary & pseudosecondary TmCO2: -58.1 – -56.6°CThCO2: 12.9 –- 30.5°CTmCLATH: 5.9 - 9.1°C ThDECREP (V): 247 – 291°CThTOT (L-V): 181 – 365°CSalinity: 1.81 – 7.54 wt%XCO2: 3 – 73 mole%XCH4: 0 – 3 mole%CO2 Density: 0.40 – 0.84 g/cm3


Primary & pseudosecondary TmCO2: -57.3 – -56.6ThCO2: 6.0 –- 30.8XCH4: 0 – 3 mole%CO2 Density: 0.53 – 0.89 g/cm3


Pseudosecondary TmICE: -9.0 - -0.3°CThTOT (L): 72 – 180°CSalinity: 1.2 – 15.0 wt%Bulk Density: 0.93 – 1.04 g/cm3

Secondary TmICE: -22.8 - -15.2°CThTOT (L): 55 – 118°CSalinity: 18.6 – 23.2 wt%Bulk Density: 1.09 – 1.17 g/cm3

Type 2


Vein Type Inclusion Type

Salinity wt% NaCl

equivNa K Mg Ca Cu Pb Zn Sr Au Ag As Sb Bi Sn W Mo Ba U Th Cs Mn Fe K/Ca

Type 2 Aq-cb 4.01.5 5841 1581

8081147660

28121564

163105

31

7550

53

59

32

4329

2013

75

2011

54

64

1814

42

11

11

2811

230133 0.56

Qz-cc alteration Aq-cb 4.511.1 8365 3638

17453704519

574384

6653

3013

10687

5657

58 1 118

1493127

3029

2014

309197

65

5544

32

32

22

3928

584384 6.34

Aq-cb 4.931.1

90762486

57032695

20462436

1314961

224133

13788

179149

116

57

76

202156

6682

7268

3014

43

78

4436

11

32

21

3450

463384 4.34

Aq 5.93.7 23888 7098

26101091662

15275

10678

197122

5433

13 3

260187

3114

Qz-cc alteration Aq 21.01.9 63998 15127

1386725491655

363390

165138 9 30

213126

419406

Type 3 Aq 20.60.8 47714 30142

9464420147

52021299

16974

1910

4937

52

22

8644

83

1015

4733

42

147

62

11

6551

16257 5.79

Type 3


Stage Style Sample No δ34S (‰)Analytical

Precision (‰) Method

1213279 -2.41 Bulk133543 -3.29 Bulk133552 -1.44 Bulk1213279 -4.14 0.006 LA1213279 -5.72 0.005 LA1213279 -6.26 0.018 LA1213279 -3.15 0.010 LA133542 -7.36 0.020 LA133542 -6.06 0.003 LA133542 -7.49 0.004 LA133542 -6.90 0.008 LA

1213226 2.03 Bulk1213226 3.77 0.220 LA1213226 0.57 0.011 LA1213226 1.50 0.003 LA1213226 2.19 0.019 LA133565 2.34 0.017 LA133565 0.58 0.009 LA

1213371 1.14 Bulk133555 -7.19 0.005 LA133555 -8.28 0.013 LA133555 -6.08 0.005 LA133555 -7.26 0.011 LA133555 -6.72 0.014 LA133555 -8.34 0.006 LA1250_12-018 -3.22 0.005 LA1250_12-018 -3.28 0.017 LA1250_12-018 -4.71 0.011 LA1213371 -3.89 0.007 LA

1149198 -2.90 Bulk1213359 -7.12 Bulk133540 -7.12 Bulk133541 -5.43 Bulk1213359 -10.61 0.031 LA1213359 -10.26 0.034 LA1213359 -9.39 0.010 LA1213359 -7.40 0.023 LA1213359 -8.55 0.007 LA1213359 -7.62 0.019 LA

Stag

e I

Stag

e II

Porp

hyry

Myl

onite

Con

tact

Frac

ture


Figure Captions

FIG. 1. Boulder-Lefroy Fault Zone with the location of the New Celebration gold deposit and other

spatially correlated gold deposits (redrawn from Eisenlohr et al., 1989)

FIG. 2a. Geology of the New Celebration gold deposit illustrating ore zones (>2.6g/t Au), diamond drill

holes sampled in this study and strike and dip of S3NC foliations within the pit. Coordinates are in local

mine grid; north arrow indicates true north. Modified from Nichols, 2003. Abbreviations; cl = chlorite; tl =

talc; cb = carbonate.

FIG. 2b. East-West cross section of the southern portion of the Hampton Boulder Jubilee deposit. The M1

plagioclase-rich porphyries form thin, ribbon-like bodies confined to the ultramafic footwall whereas

boudinaged M2 quartz-feldspar porphyry has intruded throughout the mafic-ultramafic contact, hangingwall

and footwall. Modified from Nichols, 2003

FIG. 3. Photographs and photomicrographs of illustrating the structural and timing relationships of Stage I

and Stage II gold mineralization. A. Mylonite-style mineralization. Quartz-ankerite and biotite-sericite

alteration defining S3NC foliation with syn-S3NC gold-hosting pyrite. B. Porphyry-style mineralization. Ore-

stage pyrite in syn-S3NC biotite. C. Contact-style mineralization. Coarse-grained euhedral ore-stage pyrite

overprinting S3NC foliation. D. Fracture-style mineralization. Coarse-grained pyrite in sericite veinlets

within M2 porphyry.

FIG. 4. Photographs of dominant vein types. A. Type 1 foliation-parallel quartz±calcite veins. B. Type 2

zoned quartz-calcite veins showing mutually cross-cutting relationship with S3NC foliation defined by

biotite. C. Type 3 coarse-grained quartz veins cross-cutting contact between M2 quartz-felspar porphyry

and high Mg basalt. D. Thin sericite-pyrite veins in M2 quartz-feldspar porphyry.

FIG. 5. Fluid inclusion photomicrographs from representative samples at New Celebration. A. Primary

clusters of negative crystal shaped methane fluid inclusions in calcite from type 2 quartz-calcite veins. B.

Secondary trail of irregularly shaped, single phase (at room temperature) methane inclusions in quartz from

type 2 quartz-calcite vein. C. Primary cluster of type II aqueous-carbonic inclusions in quartz from type 2

veins. Two inclusions contain a tiny rounded or triangular opaque daughter crystal. D. Transparent

nahcolite (NaHCO3) daughter crystal in primary type II aqueous-carbonic inclusions in quartz from type 2

vein. E. Type III CO2-dominant inclusion from quartz-calcite alteration associated with contact-style

mineralization. F. Secondary trail of type IV high salinity aqueous fluid inclusions in quartz from type 3

vein.

FIG 6: A. CO2 melting temperature (Tm CO2) versus CO2 homogenization temperature (Th CO2 (L)) of type

II aqueous inclusions in calcite from type 2 veins, in quartz from type 2 veins, in quartz-calcite alteration

and in quartz from type 3 veins. Inclusions in quartz from Stage I-related type 2 veins display a much wider

spread of values than those in quartz-calcite alteration and quartz from type 3 veins associated with Stage II

gold mineralization. While all fluids are relatively low in CH4, Stage II fluids contain significantly less CH4

than Stage II and have a higher density. After Neumayr and Hagemann (2002). Histograms of ThCO2 and

TmCO2 in B. type II aqueous-carbonic inclusions in calcite from type 2 veins; C. type II aqueous-carbonic

inclusions in quartz from type 2 veins; D. type II aqueous-carbonic inclusions in quartz-calcite alteration

(grey) and type 3 veins (white); E. type III carbonic inclusions from quartz in type 1 veins (hatch), quartz-

calcite alteration (grey) and type 3 veins (white).

FIG. 7. Histograms of TmCLATH or TmICE for A) primary type II aqueous-carbonic inclusions in calcite from

type 2 veins; B) primary and pseudo-secondary type II aqueous-carbonic inclusions in quartz from type 2

veins; C) type II aqueous-carbonic inclusions in quartz-calcite alteration (grey) and type 3 veins (white); D)

type IV aqueous inclusions with trace CO2 in quartz-calcite alteration (grey) and type 3 veins (white); E)

type IV low salinity aqueous inclusions without CO2 in type 1 veins (hatch), quartz in type 2 veins (black)

and type 3 veins (white); and F) secondary type IV high salinity aqueous inclusion from quartz in type 2

veins (black), quartz-calcite alteration (grey) and type 3 veins (white).

Fig. 8. Liquid- and vapor-rich end members type II aqueous-carbonic inclusions in quartz-calcite alteration

associated with fracture-style mineralization indicating phase separation.

FIG. 9. Isochors from A. type II aqueous-carbonic inclusions in calcite from type 2 veins; B. type II

aqueous-carbonic inclusions in quartz from type 2 veins associated with Stage I gold mineralization; C.

type II aqueous-carbonic inclusions in quartz-calcite alteration and type 3 veins associated with Stage II

gold mineralization; D. type III carbonic inclusions in types 1 and 3 veins, and quartz-calcite alteration; E.

type IV low salinity aqueous inclusions from types 1, 2 and 3 veins and F. type IV salinity aqueous

inclusions from types 2 and 3 veins and quartz-calcite alteration.

FIG. 10. Pressure-temperature diagram illustrating the P-T conditions of formation of different fluid

inclusion types in various vein types, the P-T path through time, the likely pressure constraints imposed by

peak metamorphism (from Spears, 1995) and the independent P-T estimate of Williams (1994) for

Southern Ore Zone mineralization at New Celebration derived from the chlorite solid-solution

geothermometer and phengite geobarometer. Interpretation of the P-T conditions recorded by the different

fluid inclusion assemblages indicate a protracted and complex fluid and tectonic history for the BLFZ.

Early fluids were emplaced in the fault at or around peak metamorphism; Stage I gold mineralization

occurred post-peak metamorphism at high temperatures and pressures. Stage II mineralization occurred

during a period of waning temperature and fluctuating pressure, possibly induced by fault valve behavior.

Late fluid assemblages (highly saline aqueous fluids, and methane-dominated fluids) were emplaced during

a period of low temperature and pressure, likely during uplift and erosion of the orogen.

FIG. 11. Total range of δ34S values from ore-related pyrite from all mineralization styles at New

Celebration (this study, Hodkiewicz, 2003) and potential sulfur sources. Vertical dashes = mean. The gray

shaded area corresponds to average δ34S values of pyrite from other Yilgarn gold deposits (summarized by

Hodkiewicz, 2003). Values for I-type granite from Ohmoto (1986), Yilgarn crust from Lambert et al.

(1984) and Archean seawater from Ohmoto and Goldhaber (1997).

FIG. 12. Hydrothermal fluid flow model for the Boulder Lefroy Fault Zone (BLFZ) at New Celebration. A.

During early D3NC ENE-WSW shortening, M1 plagioclase porphyry is emplaced into the BLFZ and

undergoes hydrothermal magnetite alteration. Methane dominated fluids of possible deep crustal or mantle

origin circulate through the fault zone. B. Stage I gold mineralization occurred at or around peak

metamorphism by wall rock sulfidation of magnetite (i) in M1 porphyries from CO2 dominated fluids of

likely metamorphic origin. C. M2 quartz-feldspar porphyries were emplaced in the BLFZ. Stage II gold

mineralization occurred due to a combination of fault-valve induced phase separation of CO2-bearing

magmatic fluids and sulfidation of iron oxides at the contact between high-magnesium basalt and M2

porphyry; D. The fault experienced a period of uplift and erosion during which highly saline fluids

potentially of magmatic origin were emplaced and the fault returned to steady state with long-lived

methane-rich fluids again dominating.

Table Captions

Table 1. Summary table of main vein type characteristics, deformation, structure and timing.

Table 2. Summary of fluid inclusion microthermometric and laser Raman data from types 1, 2 and 3 veins

and quartz-calcite alteration at New Celebration

Table 3. Average composition of fluid inclusions from different vein types at New Celebration. All

elemental concentrations are ppm. Numbers in italics are 1 standard deviation.

Table 4. Sulfur isotopic composition of pyrites from New Celebration Stage I and Stage II gold

mineralization samples.

APPENDICES

272

APPENDIX 2 Sample Data

UWA # Field #: Drill Hole Depth From

Depth To

Easting Northing Dip Azi Grid Description

140851 133541 JD236 143.20 143.35 366946.32 6565437.04 -55.0 67.77 AMG84_51 Brecciated carbonate altered quartz-feldspar phyric granite dyke140852 133542 JD236 144.00 144.25 366946.32 6565437.04 -55.0 67.77 AMG84_51 Fine-grained, foliated, carbonate-altered plagioclase-rich quartz monzonite

140853 133543 JD236 145.45 145.60 366946.32 6565437.04 -55.0 67.77 AMG84_51 Fine-grained, foliated, granular carbonated altered intermediate intrusive rock.

140854 133552 JD433 175.05 175.12 366808.17 6565594.90 -60.0 67.77 AMG84_51 Fine-grained, carbonate altered, brecciated, foliated monzonite porphyry dyke

140855 133555 HBC_1225_11 228.65 228.95 366346.13 6566263.50 -59.7 86.42 AMG84_51 Contact between metasomatized high-Mg basalt and granite porphyry dyke. Euhedral coarse-grained pyrite marks contact. High-Mg basalt is pervasively carbonate altered and strongly foliated

140856 133565 VBC_1650_9 167.60 167.77 366090.88 6566683.00 -70.2 88.82 AMG84_51 Fine-grained intensely sheared, qz-cb-bio altered, mylonitized monzonite 140857 133566 VBC_1650_9 175.04 175.22 366090.88 6566683.00 -70.2 88.82 AMG84_51 Very fine-grained, intensely sheared, quartz-carbonate altered, mylonitized

monzonite140858 133568 VBC_1650_9 194.90 195.15 366090.88 6566683.00 -70.2 88.82 AMG84_51 Contact between talc-carbonate ultramafic schist and monzonite dyke140859 133573 Pit Sample AMG84_51 Talc-carbonate altered ultramafic with relict spinifex textures140860 1149198 Pit Sample AMG84_51 Albite-carbonate altered quartz-feldspar phyric porphyry140861 1213226 VBC_1750_9 168.55 168.69 366151.53 6566784 -51.5 85.52 AMG84_51 Fine-grained mylonitized M1 monozonite. 140862 1213245 HBC_1225_13 131.10 131.40 366378.03 6566265.00 -55.5 89.02 AMG84_51 Mylonite Style Mineralisation140863 1213248 HBC_1225_13 136.20 136.50 366378.03 6566265.00 -55.5 89.02 AMG84_51 Mylonite Style Mineralisation140864 1213256 HBC_1225_13 231.25 231.45 366378.03 6566265.00 -55.5 89.02 AMG84_51 Fracture Style Mineralization140865 1213266 JD236 76.25 76.50 366946.32 6565437.04 -55.0 67.77 AMG84_51 Least Altered Hanging Wall Dolerite140866 1213279 JD236 151.45 151.70 366946.32 6565437.04 -55.0 67.77 AMG84_51 Intensely foliated, brecciated, carbonate-metasomatized biotite schist140867 1213282 JD236 130.25 130.60 366946.32 6565437.04 -55.0 67.77 AMG84_51 Porphyry Style Mineralisation140868 1213288 JD433 186.40 186.60 366808.17 6565594.90 -60.0 67.77 AMG84_51 Least Altered Ultramafic140869 1213297 JD433 192.00 192.10 366808.17 6565594.90 -60.0 67.77 AMG84_51 Porphyry Style Mineralisation140870 1213356 JD433 137.80 137.90 366808.17 6565594.90 -60.0 67.77 AMG84_51 Fracture Style Mineralisation140871 1213357 JD433 138.14 138.24 366808.17 6565594.90 -60.0 67.77 AMG84_51 Mineralized quartz-feldspar porphyry dyke140872 1213359 JD433 138.60 138.70 366808.17 6565594.90 -60.0 67.77 AMG84_51 Coarse-grained, bleached feldspar-quartz granite porphyry dyke. Brecciated

and intensely sericite altered140873 1213360 JD433 151.65 151.75 366808.17 6565594.90 -60.0 67.77 AMG84_51 Mineralized quartz-feldspar porphyry dyke140874 1213371 JD433 168.50 168.60 366808.17 6565594.90 -60.0 67.77 AMG84_51 Contact between chlorite schist and quartz-feldspar granite dyke140875 1213372 JD0433 168.80 168.90 366808.17 6565594.90 -60.0 67.77 AMG84_51 Contact between chlorite schist and quartz-feldspar granite dyke140876 1213373 JD0433 169.50 169.70 366808.17 6565594.90 -60.0 67.77 AMG84_51 Contact between chlorite schist and quartz-feldspar granite dyke140877 1213374 JD0433 172.20 172.30 366808.17 6565594.90 -60.0 67.77 AMG84_51 Mineralized plagioclase quartz monzonite140878 1213221 Pit Sample AMG84_51 Mylonitized quartz monzonite140879 HBC_1450_12-002 HBC_1450_12 282.70 282.90 366299.53 6566487.00 -70.6 84.62 AMG84_51 Least altered M2 Porphyry140880 HBC_1450_12-003 HBC_1450_12 281.40 281.50 366299.53 6566487.00 -70.6 84.62 AMG84_51 Least altered M2 Porphyry140881 HBW_1250_12-001 HBW_1250_12 183.00 183.10 366310.94 6566279.50 -66.0 86.82 AMG84_51 High-Mg basalt140882 HBW_1250_12-002 HBW_1250_12 186.20 186.50 366310.94 6566279.50 -66.0 86.82 AMG84_51 High-Mg basalt

273

UWA # Field #: Drill Hole Depth From

Depth To

Easting Northing Dip Azi Grid Description

140883 HBW_1250_12-004 HBW_1250_12 190.80 191.20 366310.94 6566279.50 -66.0 86.82 AMG84_51 High-Mg basalt 140884 HBW_1250_12-007 HBW_1250_12 213.90 214.00 366310.94 6566279.50 -66.0 86.82 AMG84_51 Carbonate-altered M1 porphyry140885 HBW_1250_12-018 HBW_1250_12 264.20 264.40 366310.94 6566279.50 -66.0 86.82 AMG84_51 Contact Style Mineralisation140886 HBW_1250_12-019 HBW_1250_12 264.50 264.60 366310.94 6566279.50 -66.0 86.82 AMG84_51 Contact Style Mineralisation140887 HBW_1250_12-022 HBW_1250_12 306.20 306.60 366310.94 6566279.50 -66.0 86.82 AMG84_51 Fracture Style Mineralization140888 HBW_1250_12-023 HBW_1250_12 307.10 307.30 366310.94 6566279.50 -66.0 86.82 AMG84_51 Fracture Style Mineralization140889 HBW_1250_12-024 HBW_1250_12 309.60 309.80 366310.94 6566279.50 -66.0 86.82 AMG84_51 Fracture Style Mineralization140890 HBW_1250_12-029 HBW_1250_12 344.50 344.80 366310.94 6566279.50 -66.0 86.82 AMG84_51 Least altered Ultramafic140891 HBW_1250_12-030 HBW_1250_12 346.80 347.00 366310.94 6566279.50 -66.0 86.82 AMG84_51 Least altered Ultramafic140892 JD0475-002 JD0475 82.00 82.30 366846.46 6565505.34 -60.0 67.77 AMG84_51 Least altered dolerite140893 JD0475-003 JD0475 95.50 96.00 366846.46 6565505.34 -60.0 67.77 AMG84_51 Qtz-cb-cl vein in dolerite140894 JD0475-005 JD0475 116.10 116.40 366846.46 6565505.34 -60.0 67.77 AMG84_51 Deformed qz-cb veins140895 JD0475-021 JD0475 208.90 209.00 366846.46 6565505.34 -60.0 67.77 AMG84_51 M1 porphyry140896 JD0475-022 JD0475 211.70 211.90 366846.46 6565505.34 -60.0 67.77 AMG84_51 M1 porphyry140897 JD0475-024 JD0475 223.60 223.80 366846.46 6565505.34 -60.0 67.77 AMG84_51 M2-Mafic contact140898 133570 Pit Sample Qz-bio-ank mylonite with disseminated pyrite and late magnetite140899 1213365 JD0433 154.75 154.86 366808.17 6565594.90 -60.0 67.77 AMG84_51 Mineralized quartz-feldspar porphyry dyke

274

APPENDICES

275

APPENDIX 3 Petrographic Descriptions

133541 UWA Number: 140851Drill Hole ID: JD236 Depth: 143.20-143.35

% Mineral Description60 qz

35 plg

3 cb

1 py

1 bio

tr sl

tr gl

% Mineral Description90 qz10 cb

qz veinscb altnpyritebio

Sketches & Photographs

fine elongate tabular grains defining very weak foliation.fine-grained anhedral grains occurring as inclusions in pyrite. Some show chalcopyrite disease. Yellow internal reflections- Fe-poor

Sample No:

Description:

coarse-grained (20-50µm) anhedral carbonate grains forming patches in the groundmasscoarse-grained (50-100µm) subhedral pyrite grains occupying sericite-chlorite filled fractures cross-cutting quartz veins

Brecciated carbonate altered quartz-feldspar phyric granite dyke

fine-grained anhedral recrystallized interlocking quartz forming large (20-30µm) euhedral plagioclase phenocrysts altered (saussuritised) to sericite-carbonate

Host Rock Mineralogy:

rare rounded galena blebs occurring as inclusions hosted within pyrite.

fine-grained to coarse-grained polycrystalline quartz forming coarse-grained anhedral patches intergrown with quartz

Pyrite grains are dirty, inclusion rich and form aggregates developing in fractures occupied by sercite±chlorite. No gold observed in this sample. Silicates, sphalerite, galena form inclusions within pyrite

Vein Mineralogy:

Paragenesis:

Comments:

276


% Mineral Description60 plg12 cb

15 bio

10 qz

2 py

tr sl

tr cpy

tr Au


40 cb


Rare anhedral sphalerite grains, disseminated although sometimes occurring with pyrite

Coarse-grained anhedral carbonate predominantly occurring qz-cb veins S3NC (bio+py+slf) later qz±cb veins

S3NC foliation defined by aligned biotite laths. Plagioclase show partial alignment with foliation. Pyrite intimately associated with biotite - syn D3NC

Comments:

Rare tiny anhedral grains, disseminated, possibly associated with Au

Sample No:

Description: Fine-grained, foliated, carbonate-altered plagioclase-rich quartz monzonite


Coarse-grained euhedral (cubic) to subhedral grains, often with inclusions. Possibly zoned. Grains are typically enclosed within biotite bands or have biotite crystals growing parallel to grain boundaries synchronous with foliation

Fine-grained euhedral plagioclase laths form bulk of rock. Fine-grained anhedral carbonate forming masses which overprint fabric - lateEuhedral elongate crystal forming bands and defining foliation planes. Grains wrap around pyrite grains and also along edges of early quartz-carbonate veins.Minor anhedral quartz, medium grained, interlocking. Form patches which may be relict veins or recrystallized quartz alteration.

Paragenesis:

Vein Mineralogy:

Very tiny grain adjacent to chalcopyrite crystal

Coarse-grained anhedral polycrystalline qz veins. Occur sub-parallel/oblique to foliation but are edged by aligned biotite grains. Possibly two quartz vein stages - early qz-cb, later

277


% Mineral Description50 plg30 cb

3 bio

7 py

10 qz

tr sl

tr Au

% Mineral Description99 qz1 cb


Sample No:

Description: Fine-grained, foliated, granular carbonated altered intermediate intrusive rock.


Fine-grained, euhedral tablar crystals, partially aligned with Fine-grained subhedral intergranular carbonate. Also occurs defining foliation planesFine-grained elongate platy crystals partially developing bands foliation. Borders quartz veins. Bimodal pyrite distribution. Fine-grained euhedral intergranular pyrite and coarse-grained subhedral pyrite associated with biotite bands. Some pyrite zoned with dirty inclusion-rich cores and clean inclusion-free rimsFine-grained granular quartz, possibly relict veins. Occur approximately parallel to foliationTiny anhedral sphalerite grains disseminatd through matrix and also occurring as inclusions within pyriteSmall grain hosted within pyrite on edge of silicate inclusion

Paragenesis:

Comments:

Vein Mineralogy:

early qz veins S3 (bio-qz-cb-py)

Anhedral, granular interlocking quartzSmall, anhedral, intergranular

Foliation defined by partial alignment of feldspar and byn qz-cb-bio-py bands. Possible early quartz veins. Bimodal pyrite distribution - two separate events. Large pyrite hosting Au zoned.

278


% Mineral Description60 plg

20 cb15 bio5 py


49 cb1 py


Comments: Thick quartz vein sub-parallel to foliation - both appear to be showing mutually cross-cutting relationships vein possibly D3. Narrow quartz vein cross-cuts foliation and thick vein

Sample No:

Description: Fine-grained, carbonate altered, brecciated, foliated monzonite porphyry dyke


Patchy fine-grained carbonate overprinting groundmassFine-grained tabular biotite forming bands defining foliation

Fine-grained plagioclase laths occurring both as a phenocryst phase and as groundmass. Phenocrysts are partially aligned with foliation

Coarse-grained euhedral-subhedral disseminated pyrite.

Paragenesis:

Coarse-grained, subhedral interlocking grains with carbonate Fine-grained, sugary, intergrown with quartz in composite veins.

Vein Mineralogy:

Coarse-grained euhedral grains intergrown with qz-cb veins

279

133555 UWA Number: 140855Drill Hole ID: HBC_1225_11 Depth: 228.65-228.95

Granite dyke

% Mineral Description40 cb

25 plg

30 qz5 ser

2 py

tr bio

High-Mg basalt


15 ser

5 py

tr bio

tr sltr Autr cpy

% Mineral Descriptionpy

ser

qz

biocb

tr Autr gn

Coarse-grained subhedral grains, somewhat elongate, preferentially occurring with sericite bands and showing a preferred orientation. Grains are typically dirty and are zoned with an inclusion-free rim and and inclusion-rich core. Some grains show oscillatory zoning.Fine-grained platy crystals rimming pyrite grains and intergrown with sericite

Contact between metasomatized high-Mg basalt and granite porphyry dyke. Euhedral coarse-grained pyrite marks contact.

fine-grained anhedral interlocking grains. Forms bands of different grain size. Occurs predominantly in association with sericite

Massive coarse-grained pyrite grains at contact between high-Mg basalt and granite porphyry. Grains are anhedral, commonly contain abundant inclusions

Medium-grained, predominantly subhedral grains showing ecidence of saussuritization. Some grains show relict lath shape but most have been partially recrystallized. Relict twinning evident in some grainsFine-grained anhedral recrystallized quartz groundmass.Fine-grained acicular grains forming bands intergrown with carbonate. Rare radiating fans overgrowing groundmassFine-grained anhedral-subhedral disseminated pyrite occassionally rimmed by fine-grained platy biotiteFine-grained platy crystals usually occurring intergrown with sericite but also rimming pyrite grains

Fine-grained to coarse-grained anhedral carbonate pervasively altering sample

Sample No:

Description:



Fine-grained platy sericite showing preferred orientation, aligned, defines foliation. Small platy grains also occur in intergranular spaces with carbonate

Fine-grained subhedral grains occurring adjacent to pyriteRare tiny rounded inclusions within pyrite grains

Mineralized Contact:

Rare tiny anhedral grains developing on pyrite grain

Occurs as small rounded inclusions in pyrite or as larger Rare anhedral grains, disseminated

Medium-grained anhedral recrystallized quartz intergrown with pyrite, sericite, biotite and carbonateMinor fine-grained platy biotite intergrown with sericiteCoarse-grained anhedral grains overprinting quartz

Fine-grained anhedral aligned sericite rims and is intergrown with pyrite

280

% Mineral Descriptiontr sl

tr mt


Mineralized Contact:

High Mg basalt is texturally and compositionally zoned - bands of coarse-grained carbonate alternate with fine-grained bands, and with sericite, which defines foliationFoliation is defined by anastamosing sericite bandsContact is characterized by intense sulfidation (py±sl±gn) and sericite alteration

Au only occurs on high-Mg basalt side of contactProximal granite porphyry does not show any foliation

Au is predominantly hosted as inclusions within pyrite, but also occurs along pyrite grain boundaries and rarely as free grains in groundmass

Paragenesis:

Comments:

Rare anhedral grains either disseminated in groundmass or as inclusions within pyriteRare anhedral grains either disseminated in groundmass or as inclusions within pyrite

281

133565 UWA Number: 140856Drill Hole ID: VBC_1650_9 Depth: 167.60-167.77


35 cb

20 bio

7 mt

3 py

% Mineral Description8020

qzcb

Magnetite syn-D3NC


Sample No:

Description: Fine-grained intensely sheared, qz-cb-bio altered, mylonitized monzonite

Fine-grained subhedral to euhedral carbonate forms groundmass with interlocking quartz grains. Larger subhedral grains occur in quartz-carbonate "boudins"


Fine-grained anhedral recrystallised quartz comprises groundmass. Minor larger interlocking quartz grains form foliation-parallel "boudins" with coarse-grained carbonate possibly relict early veins

Fine-grained to medium-grained prismatic crystals forming bands and defining foliationFine- to medium-grained. Occurring with biotite along foliation planes. Commonly replaced by pyrite

Paragenesis:

Fine-grained to medium-grained anhedral to subhedral pyrite developed with biotite along foliation planes. Replacing magnetite

Wide (5mm) clear quartz carbonate veins obliquely cross-cutting foliation. Grains are coarse and interlocking. Vein shows minor displacement of foliation planes suggesting that formation was contemporaneous with D3NC

Comments:

Vein Mineralogy:

Foliation parallel quartz-carbonate boudin veins possibly pre-D3NC

282


283

133566 UWA Number: 140857Drill Hole ID: VBC_1650_009 Depth: 175.04-175.22


25 bio

40 cb

3 cl

2 mt

tr py

% Mineral Description80 qz17 cb3 cl

At least two pyrite populations in this sample. Fine-grained sub-euhedral pyrite occurs disseminated in groundmass approximately conformable with foliation ie. syn-D3NC. Coarse-grained euhedral pyrite overprints foliation (post D3NC).

Large euhedral-subhedral dirty grains with numerous inclusions including magnetite, pyrrhotite and chalcopyrite

Fine-grained, elongate, euhedral prismatic biotite delineating foliation planesFine-grained sub-euhedral prismatic grains intergrown with quartz and forming groundmass. Grains show some alignment with foliationRare anhedral-subhedral elongate grains (10-20µm) occurring sub-parallel to foliationFine-grained, subhederal, possibly two stages - anhedral grains (10-20µm) overprinting fabric and finer-grained anhedral grains (2-4µm) preferentially occuring with biotite along foliation planes

Fine-grained chlorite forming thin chlorite-carbonate veinlet

Thick quartz vein appears to be approximately synchronous with D3NC foliation. Vein mostly crosscuts foliaton but in places is offset by it

Paragenesis:

Comments:

Vein Mineralogy:

qz-cb boudins D3NC+qz-cb veins cl-cb veinlets

Strong foliation delineated by aligned prismatic biotite grains and quartz. Small islands of coarser-grained interlocking quartz±carbonate form foliation-parallel boudins

Coarse-grained (15-20µm) subhedral interlocking quartz Coarse-grained (15-20µm) euhedral interlocking carbonate,

Two apparent magnetite stages - early, fine-grained, incorporated into biotite foliation bands, and later, coarser grained, overprinting fabric.

Sample No:

Description:


Very fine-grained, intensely sheared, quartz-carbonate altered, mylonitized monzonite

Fine-grained, anhedral recrystallized quartz, intergrown with carbonate and forming groundmass. Minor larger grains, anhedral, interlocking, forming foliation parllel quartz "boudins", possibly relict pre-D3NC veins

284


A B

A

B

285

1213226 UWA Number: 140861Drill Hole ID: Depth:


40 qz

15 bio5 py

tr ab

tr mt


qzcb


Sample No:

Description: Fine-grained mylonitized M1 monzonite. Foliation defined by aligned quartz-carbonate bands and anastamosing biotite

Fine-grained clear quartz intergrown with carbonate forms foliation. Medium-grained white quartz forms "boudin" veins -


Fine-grained cream-brown (ankerite) grains form laminae with fine-grained quartz and define S3NC foliation.

Forms anastamosing bands, defines S3NC foliationPossibly two populations - fine-grained anhedral pyrite disseminated throughout sample but typically forming along foliation planes, preferentially occurring with biotite laminae, and coarse-grained subhedral to euhedral pyrite overprinting foliation.Fine-grained pink (alteration halo) adjacent to quartz±carbonate vein. Only observed where vein intersects biotite laminae

Comments:

Vein Mineralogy:

Early quartz veins S3NC + qz-cb veins + py mt +py

Fine-grained aggregates of anhedral magnetite overprinting foliation

Wide (1-7mm) clear qz±cb vein cross-cutting foliation. Veins are partially deformed, foliation planes partially curve into veins in some places. Texturally appear to be synchronous with foliation (syn D3NC)

Paragenesis:

286


287


% Mineral Description30 ank

40 bio

20 qz10 py


100 qz


Sample No:

Description: Intensely foliated, brecciated, carbonate-metasomatized biotite schist

Fine-grained, elongate play grains, form long lines delineating foliation planes


Fine-grained subhedral ankerite, forms froundmass with recrystallised quartz and albite/plagioclase. Shows some preferred orientation

Fine-grained recrystallised quartz groundmassCoarse-grained euhedral-anhedral pyrite, possibly two generations. Very large anhedral grains, flattened, elongate, occur with biotite in foliation planes. Finer grained euhedral pyrite overprints fabric

Thin veins of clear to milky quartz, occur parallel to foliation. Veins have been boudinaged and are edged with biotite

Vein Mineralogy:

Ptygmatic clear coarse-grained quartz veins showing mutually cross-cutting relationships with foliation. Veins have been deformed and fractured where they intersect foliation. Syn-D3NC. Surrounded by carbonate alteration halo

Sample intensely pervasively carbonate-quartz alteredTwo pyrite generations - early, coarse-grained, dirty, syn-D3NC, Au-related, and late, finer grained, cubic, overprinting fabric

Paragenesis:

Comments:

288


289

1213359 UWA Number: 140873Drill Hole ID: Depth:

% Mineral Description40 fsp

30 qz

30 sertr py


10 py


Fine-grained sericite altering from feldspar. PervasiveRare coarse-grained disseminated euhedral pyrite

Paragenesis:

Sample No:

Description: Coarse-grained, bleached feldspar-quartz granite porphyry dyke. Brecciated and intensely sericite altered

Coarse-grained interlocking quartz overprinting primary porphyritic texture


Matrix predominantly alkali feldspar. Relict phenocryst laths observed in quartz alteration. Feldspar altering to sericite

Comments:

Vein Mineralogy:

Several quartz vein phases, wide (1-5mm) clear white bucky quartz veinsThick py±qz veins cross cutting breccia. May themselves be crosscut by later thin quartz veins but relationship is unclear. Pyrite is coarse-grained, massive within vein

Porphyry has been completely bleached and altered. No primary mafic minerals remain. Quartz has extensively overprinted primary minerals and fabric; only rare phenocrysts remain. Matrix has been pervasively altered to sericite (and albite).

290

HBW_1250_12-004 UWA Number: 140884Depth: 190.8-191.2


20 bio

7 py

3 mt

Vein 1

% Mineral Description955tr

qzcl

bio

Vein 2


qzpy

Narrow (1-2mm) single stage opening fracture vein. Quartz dominant but where


Sample No:

Description: Fine-grained, dark green-grey massive magnetic high-Mg basalt. Weakly brecciated with several vein sets


Fine-grained, anhedral with diffuse grain boundaries. Intergrown with biotite

Vein Mineralogy:

Vein Mineralogy:

Narrow (2-5mm) diffuse deformed zoned qz-cl±bio veins. Chlorite on edges of growth zones (multiple opening veins). Biotite typically associated with chlorite. Possible trace sericite.

Paragenesis:

Comments: Both vein sets appear to crosscut magnetite(±pyrite) alteration events. In core, magnetism decreases with increasing vein intensity

Fine to medium-grained, subhedral, typically stubby grains. Likely altered from amphibole or pyroxene. Fine-grained, anhedral, disseminated. Overprints matrixFine-grained, anhedral, disseminated. Also overprints matrix

291

HBW_1250_12-018 UWA Number: 140886Drill Hole ID: HBW_1250_12 Depth: 264.2-264.4


30 bio

20 cb

7 py


cbfc


Sample No:

Description: Fine-grained, dark grey strongly sheared, brecciated carbonate-pyrite-fuchsite altered high Mg basalt.

Fine-grained, platy. Defines shear planes in sample. Edges some deformed carbonate veins.


Fine-grained anhedral diffuse grain boundaries, likely almost completely carbonate (albite) altered. Forms boudinaged domains between biotite-rich shear planes ie. rock compositionally zoned.

Paragenesis:

Comments:

Fine-grained light brown (ankerite?). Occurs as alteration of plagioclase and as narrow halo around some carbonate veins. Alteration patchy, variable intensity. Intensity increases adjacent to thin deformed qz-cb veinsCoarse-grained, anhedral. Typically occurs with biotite along shear planes and against margins of thick deformed calcite veins. Grains commonly deformed. Do not occur in thick calcite veins but do overprint thin quartz-carbonate veins

Vein Mineralogy:

Thin-thick (3mm->50mm) carbonate-fuchsite veins. Deformed, wrapped by shear fabric. Commonly have carbonate (ankerite)±fuchsite alteration halo of variable with and intensity. Veins are typically rimmed by biotite+pyrite but pyrite is rarely observed within the vein

292

HBW1250_12-019 UWA Number: 140887Drill Hole ID: HBW1250_12 Depth: 264.4-264.6

Granite Porphyry


4 fc

1 py

45 qz

High-Mg basalt

% Mineral Descriptionplg

bio

cb

10 py

% Mineral Descriptionqzcbpyfc

Sample No:

Description: High-Mg basalt - M2 granite porphyry contact. Both units highly atered and sheared. Pyrite abundant at contact, decreasing with decreasing proximity to contact. Mgb strongly biotite-carbonate altered; Fp strongly carbonate-fuchsite altered. Coarse-grained carbonate-fuchsite vein occupies immediate contact. Primary ingnous textures in both Mgb and Fp destroyed

Fine-grained, platy. Defines shear planes. Forms compositional zones with altered plagioclase


Light brown finegrained ankerite intergrown with calcite and quartzFine-grained, elongate. Defines shear planes in granite porphyryTrace anhedral medium grained pyrite. Occurs with fuchsite along foliation planesFine-grained, intergrown with carbonate completely altering primary mineralogy

Comments:

Vein Mineralogy:

Thick laminated sheared vein parallel to contact. Calcite is fine-grained, subhedral, interlocking. Intergrown with rare anhedral clear quartz grains. Fuchsite forms trails parallel to shear and contact, pyrite coarse-grained, anhedral, deformed and occurs exclusively along fuchsite planes within vein


Paragenesis:

Fine-grained, euhedral. Dark brown (ankerite). Patchy alteration, typically adjacent to quartz-carbonate veinsCoarse-grained, anhedral, commonly deformed. Typically occurs with biotite along shear planes and wraps around thick calcite veins. Rarely overprints veins and decreases in abundance where carbonate alteration is most intense

Fine-grained, anhedral, diffuse grain boundaries. Mostly altered to carbonate and albite

293


294

HBW_1250_12_22 UWA Number: 140888Drill Hole ID: HBW_1250_12 Depth:

% Mineral Description30 ksp

65 ab

5 cb

tr pytr qz


qzpyseropq

Fine-grained, anhedral, disseminated throughout albite groundmassFine-grained, euhedral, disseminated

Vein Mineralogy:

Rare rounded coarse-grained (2-3mm) quartz phenocrysts

Sample No:

Description: Coarse-grained K-feldspar phyric granite seriate porphyritic dyke. Strong percasive carbonate-albite-(hematite) alteration. Weakly brecciated.

Pervasively altered groundmass. Very fine-grained, can't distinguish individual grains


Medium- to coarse-grained (0.5-2.0mm) anhedral grains. Albitised

Thin (2-5mm) clear quartz breccia veins. Coarse-grained quartz, euhedral, interlocking.

Paragenesis:

Comments:

Thin (1-2mm) dark veins, which crosscut vein 1. Veins have dark edge with chlorite or opaque mineral and clear quartz centre. May be quite thick, or thin out to ser-py veins only. Pyrite is fine- to medium-grained and euhedral. May contain gold.


295


% Mineral Description40 ksp

58 ab2 cbtr py


qzbioser

ab-cb bx bio-qz

Sample No:

Description: Brecciated pervasively carbonate-albite altered seriate porphyritic quartz-K-feldspar granite dyke

Thick (5-50mm) zoned breccia veins. Biotite fine grained, platy, typcially rims vein. Quartz coarse-grained, granular, interlocking. Sericite rare, coarse-grained, anhedral, interlocking with quartz. No alteration halo.


Coarse-grained, anhedral to euhedral. Seriate grain size distribution. Rare zoned phenocrysts. Strong pervasive albite alteration

Paragenesis:

Comments:

Vein Mineralogy:

Very fine grained pervasively altered groundmassFine-grained anhedral, disseminated throughout groundmassFine-grained, euhdral, disseminated


296


High Mg basalt

% Mineral Description25 bio

50 plg

15 cb

10 py

M2 Porphyry

% Mineral Description55 ab40 ksp

5 bio

tr pytr cb

Vein 1


Vein 2


qzcbser

Rare fine- to medium-grained subhedral to anhedral pyrite

Vein Mineralogy:

Thin zoned veins, 1-2mm wide. Undeformed. Typically fine- to medium-grained, outer carbonate-sericite, inner quartz. Commonly have narrow alteration halo. May contain trace Au in outer carbonate zone?

Vein Mineralogy:

Sample No:

Description: Contact between M2 granite porphyry and high Mg basalt. Basalt is fine-grained, massive, pervasively strongly to intensely biotite-carbonate-pyrite altered. Pyrite is coarse-grained, euhedral, disseminated, although at contact is less idiomorphic than other pyrite. M2 granite porphyry is coarse-grained, K-feldspar-phyric. Phenocrysts are subhedral, fractured. Unit is intensely albite altered. Late thick undeformed quartz veins with no alteration halo cut contact

Fine-grained, subhedral, typically forms clusters. Partially altered to albite. Partially intergrown with biotite and carbonate


Very fine grained, forms groundmass. Likely alteration of primary mafic phases. Platy, commonly edges quartz-carbonate-sericite veins. Increases in abundance at M2-Mgb contact


Moderate patchy ankerite alteration overprinting plagioclase-biotite groundmass. Typically associated with quartz-carbonate-sericite veinsCoarse-grained euhedral-cubic disseminated pyrite overprinting groundmass. Rarely overprints ceins. Rare skeletal grains. Increased abundance at M2-Mgb contact

Rare patchy carbonate overprinting fabric

Fine-grained, opaque milky quartz veins. Deformed, possibly pre-D3NC. Rare. Crosscut by contact

Very fine-grained, forms ground massSubhedral to euhedral feldspar laths. Some appear partially resorbed. Coarse-grained. Rare fractured grainsFine-grained, typically forming thin stringers into porphyry perpindicular to contact

297

Vein 3


Vein 4

% Mineral Description955trtr

serpyclAu

Vein 1 intrusion vein 2 vein 3 vein 4


Vein Mineralogy:

Wide massive buck quartz veins. Cross-cut contact and S3NC foliation

Thin fine-grained sericite stringers which crosscut veins 2 and 3

Paragenesis:

Comments:

Vein Mineralogy:

298

JD0475-003 UWA Number: 140896Drill Hole ID: JD0475 Depth: 95.5-96.0


25 bio

5 cc

tr py


cbclqz


Paragenesis:

Comments:

Vein Mineralogy:

Fine-grained platy grains replacing primary mafic minerals. Rare larger clusters. Intergrown with plagioclaseMedium grained white anhedral grains. Typically replace plagioclase but may also replace mafic minerals. May occur with biotite rimming replaced mafic mineralFine-grained anhedral disseminated pyrite overprints fabric

Wide (>30mm) replacement vein with diffuse vein margins. Vein is fibrous and minerals are oriented oblique to vein. Calcite and chlorite are fine-grained, fibrous; quartz is fine-grained, anhedral, with no preferred orientation. Vein has wide calcite-chlorite halo, also with preferred orientation - sheared or deformed vein

Sample No:

Description: Dark green, fine-grained cumulate dolerite. Unit is moderately pervasively carbonate altered and primary mafic minerals


Fine-grained euhedral stubby laths, cumulate, interlocking with mafic minerals. Pervasively carbonate altered.

299

JD075-005 UWA Number: 140897Drill Hole ID: JD075 Depth: 116.1-116.4


10 bio

10 cb

10 mt

5 cl

15 act

tr py


ccclpy


Sample No:

Description: Dark grey-green, fine- to medium-grained massive dolerite. Unit has been moderately pervasively carbonate altered and primary mafic minerals are biotite±carbonate altered. Actinolite


Fine-grained subhedral plagioclase, percasively carbonate altered. Cumulate matrix

Paragenesis:

Comments:

Vein Mineralogy:

Fine-grained euhedral, platy. Typically occurs partially replacing primary mafic minerals - relict phenocryst shapes observed. Fine-grained, anhedral. Often skeletal, with magnetite cores. Possibly replacing phenocrystsFine-grained, anhedral, granular. Typically occurs with carbonate as cores to skeletal calcite grains but also occurs along edges of carbonate-chlorite veinsFine-grained, anhedral, typically occurs with carbonate in carbonate-chlorite±quartz vein halosCoarse-grained, acicular. Randomly oriented, overprinting fabricFine-grained, anhedral, disseminated

Wide (2-20mm) weakly deformed breccia veins. Calcite fine-grained, granular, interlocking. Chlorite fine-grained subhedral, forms patches and zones in vein. Vein partially zoned, possibly multiple stage opening vein. Veins have narrow carbonate-chlorite alteration halo. Trace pyrite (fine-grained, anhedral) always associated with chlorite

300


301

APPENDICES

302

APPENDIX 4 Fluid Inclusion Microthermometry

H2O-CO2-CH4-NaCl

Sample No.

Min

Stage Min Style Vein Type

Inclusion

type No

1213279 1 Porphyry 2 aq-cb 9 -57.34 ± 0.30 7.8 ± 0.70 12.1 ± 3.2 1.03 ± 0.01 0.76 ± 0.23 4.24 ± 1.21 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 6 -56.60 ± 0.10 7.8 ± 0.40 15.8 ± 3.1 1.03 ± 0.01 0.77 ± 0.14 4.28 ± 0.71 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 5 -59.30 ± 1.70 8.3 ± 0.70 16.1 ± 5.2 1.02 ± 0.01 0.59 ± 0.23 3.32 ± 1.22 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 4 -58.00 ± 0.50 8.3 ± 0.10 21.7 ± 1.7 1.02 ± 0.00 0.61 ± 0.04 3.40 ± 0.22 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 4 -59.50 ± 1.70 9.3 ± 0.60 14.9 ± 4.3 1.00 ± 0.01 0.25 ± 0.19 1.46 ± 1.08 0.00 ± 0.00

1213279 1 Porphyry 2 aq-cb 4 -59.50 ± 1.70 8.7 ± 0.60 14.3 ± 5.1 1.01 ± 0.01 0.49 ± 0.19 2.80 ± 1.02 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 4 -57.00 ± 0.20 7.4 ± 0.30 19.4 ± 2.3 226.4 ± 0.5 1.03 ± 0.00 0.89 ± 0.10 4.93 ± 0.53 0.02 ± 0.00

1213279 1 Porphyry 2 aq-cb 4 -56.90 ± 0.30 7.0 ± 0.40 16.6 ± 1.7 239.9 ± 9.6 1.04 ± 0.00 1.04 ± 0.13 5.72 ± 0.68 0.02 ± 0.00

1213279 1 Porphyry 2 aq-cb 3 -56.80 ± 0.10 7.7 ± 1.20 19.9 ± 1.3 226.4 ± 0.5 352.3 1.03 ± 0.02 0.78 ± 0.39 4.33 ± 2.07 0.01 ± 0.01

1213279 1 Porphyry 2 aq-cb 3 -58.80 ± 2.10 7.3 ± 0.10 12.4 ± 3.9 1.03 ± 0.00 5.21 ± 0.20 0.02 ± 0.00

1213279 1 Porphyry 2 aq-cb 2 -57.50 ± 0.10 7.8 ± 0.30 17.2 ± 0.1 1.03 ± 0.00 0.76 ± 0.10 4.25 ± 0.51 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 5 -56.60 ± 0.00 7.1 ± 0.90 23.4 ± 1.0 1.03 ± 0.01 0.99 ± 0.31 5.47 ± 1.61 0.02 ± 0.01

1213279 1 Porphyry 2 aq-cb 6 -56.90 ± 0.30 7.8 ± 0.50 20.7 ± 4.0 262.3 ± 15.2 329.0 ± 0.4 1.03 ± 0.01 0.78 ± 0.15 4.34 ± 0.82 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 2 -58.90 ± 1.80 8.4 ± 0.00 11.9 ± 2.9 277.2 1.02 ± 0.00 0.56 3.15 ± 0.00 0.01 ± 0.00

1213279 1 Porphyry 2 aq-cb 9 -56.70 ± 0.00 8.6 ± 0.50 29.6 ± 0.7 267.2 ± 0.4 269.6 ± 1.0 1.01 ± 0.01 0.47 ± 0.18 2.67 ± 0.99 0.01 ± 0.00

HBW_1250_12-018 2 Contact qz-cb altn aq-cb 6 -57.10 ± 0.50 7.9 ± 0.00 23.6 ± 3.3 1.02 ± 0.00 0.69 ± 0.01 3.92 ± 0.07 0.01 ± 0.00

HBW_1250_12-018 2 Contact qz-cb altn aq-cb 1 -56.60 7.3 17.9 1.03 0.93 5.15 0.02

HBW_1250_12-018 2 Contact qz-cb altn aq-cb 6 -56.60 7.0 ± 0.60 15.0 ± 1.9 186.4 1.04 ± 0.08 1.04 ± 0.20 5.73 ± 1.01 0.02 ± 0.00

HBW_1250_12-018 2 Contact qz-cb altn aq-cb 5 -56.60 8.1 ± 0.17 30.7 ± 0.0 304.0 ± 16.7 1.02 ± 0.00 0.64 ± 0.06 3.63 ± 0.31 0.01 ± 0.00

1213359 2 Fracture 3 aq-cb 5 -57.00 ± 0.44 7.4 ± 0.89 24.3 ± 6.1 1.03 ± 0.01 0.90 ± 0.30 4.98 ± 1.59 0.02 ± 0.01

1213359 2 Fracture 3 aq-cb 3 -57.10 ± 0.20 7.4 ± 0.55 29.2 ± 2.1 1.03 ± 0.01 0.91 ± 0.19 5.03 ± 0.99 0.02 ± 0.00

1213359 2 Fracture 3 aq-cb 4 -56.60 8.0 ± 0.38 15.8 ± 3.4 1.02 ± 0.01 0.68 ± 0.13 3.84 ± 0.70 0.01 ± 0.00

1213359 2 Fracture 3 aq-cb 4 -56.67 ± 0.60 8.6 ± 0.40 14.9 ± 0.8 247.0 297.0 ± 21.8 1.01 ± 0.01 0.49 ± 0.14 2.76 ± 0.77 0.01 ± 0.00

1213359 2 Fracture 3 aq-cb 1 -58.00 8.2 24.8 1.02 0.62 3.52 0.01

1213359 2 Fracture 3 aq-cb 1 -58.10 8.2 27.6 1.02 0.62 3.52 0.01

133541 2 Fracture 3 aq-cb 7 -56.60 7.3 ± 0.21 22.4 ± 1.7 1.03 ± 0.00 0.93 ± 0.07 5.15 ± 0.37 0.02 ± 0.00

133541 2 Fracture 3 aq-cb 5 -56.60 ± 0.00 7.0 ± 0.10 24.2 ± 1.3 1.04 ± 0.00 1.03 ± 0.03 5.68 ± 0.17 0.02 ± 0.00

133541 2 Fracture 3 aq-cb 4 -56.60 ± 0.00 7.2 ± 0.20 22.2 ± 3.5 1.03 ± 0.00 0.97 ± 0.07 5.39 ± 0.37 0.02 ± 0.00

133541 2 Fracture 3 aq-cb 8 -56.60 ± 0.00 7.1 ± 0.30 22.9 ± 0.9 1.03 ± 0.01 1.00 ± 0.12 5.53 ± 0.60 0.02 ± 0.00

133541 2 Fracture 3 aq-cb 15 -56.61 ± 0.00 7.2 ± 0.60 23.9 ± 2.6 1.03 ± 0.01 0.95 ± 0.20 5.23 ± 1.03 0.02 ± 0.00

133541 2 Fracture 3 aq-cb 13 -57.82 ± 0.00 7.4 ± 0.30 24.8 ± 2.7 276.6 ± 20.6 301.2 ± 10.8 1.03 ± 0.00 0.91 ± 0.10 5.05 ± 0.53 0.02 ± 0.00

Tm CO2 Tm Clath Th CO2 L-V Th Crep Th Total Aq Density Molal NaCl Wt% NaCl X(NaCl)

303

H2O-CO2-CH4-NaCl

Sample No.

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

1213279

HBW_1250_12-018

HBW_1250_12-018

HBW_1250_12-018

HBW_1250_12-018

1213359

1213359

1213359

1213359

1213359

1213359

133541

133541

133541

133541

133541

133541

0.82 ± 0.03 52.92 ± 1.71 0.97 ± 0.01 0.03 ± 0.01 0.78 ± 0.05 0.20 ± 0.05 0.011 ± 0.003 0.01 ± 0.00 0.94 ± 0.01 25.36 ± 1.52

0.81 ± 0.03 54.10 ± 1.78 1.00 ± 0.00 0.00 ± 0.00 0.80 ± 0.03 0.19 ± 0.03 0.011 ± 0.001 0.00 ± 0.00 0.94 ± 0.01 25.06 ± 0.99

0.71 ± 0.08 62.78 ± 7.10 0.92 ± 0.06 0.08 ± 0.06 0.88 ± 0.01 0.10 ± 0.01 0.009 ± 0.004 0.01 ± 0.01 0.93 ± 0.02 23.00 ± 0.26

0.65 ± 0.13 70.12 ± 15.59 0.96 ± 0.03 0.04 ± 0.03 0.87 ± 0.05 0.11 ± 0.05 0.009 ± 0.001 0.01 ± 0.01 0.88 ± 0.11 24.71 ± 4.73

0.67 ± 0.05 63.54 ± 6.03 0.89 ± 0.07 0.11 ± 0.07 0.88 ± 0.04 0.10 ± 0.03 0.004 ± 0.003 0.01 ± 0.02 0.92 ± 0.01 23.10 ± 1.51

0.68 ± 0.11 64.03 ± 13.17 0.89 ± 0.02 0.11 ± 0.02 0.83 ± 0.05 0.14 ± 0.04 0.008 ± 0.002 0.02 ± 0.01 0.88 ± 0.10 25.85 ± 4.51

0.77 ± 0.01 56.63 ± 0.77 0.99 ± 0.01 0.01 ± 0.01 0.69 ± 0.29 0.30 ± 0.29 0.011 ± 0.005 0.01 ± 0.01 0.91 ± 0.06 29.70 ± 11.11

0.80 ± 0.02 54.57 ± 1.31 0.99 ± 0.01 0.01 ± 0.01 0.75 ± 0.03 0.23 ± 0.03 0.014 ± 0.002 0.00 ± 0.00 0.93 ± 0.02 26.56 ± 1.36

0.76 ± 0.00 57.20 ± 0.00 0.99 ± 0.00 0.01 ± 0.00 0.69 ± 0.10 0.30 ± 0.11 0.010 ± 0.006 0.00 ± 0.00 0.88 ± 0.03 29.92 ± 4.18

0.69 ± 0.19 62.26 ± 14.02 0.90 ± 0.10 0.10 ± 0.10 0.80 ± 0.05 0.17 ± 0.06 0.014 ± 0.002 0.02 ± 0.01 0.90 ± 0.06 26.00 ± 1.70

0.76 ± 0.01 56.99 ± 0.30 0.97 ± 0.00 0.03 ± 0.00 0.53 ± 0.40 0.44 ± 0.39 0.008 ± 0.006 0.01 ± 0.01 0.86 ± 0.09 35.84 ± 15.47

0.73 ± 0.01 60.01 ± 1.06 1.00 ± 0.00 0.00 ± 0.00 0.83 ± 0.05 0.16 ± 0.05 0.015 ± 0.005 0.00 ± 0.00 0.92 ± 0.03 24.78 ± 1.99

0.75 ± 0.05 58.21 ± 4.65 0.99 ± 0.01 0.01 ± 0.01 0.76 ± 0.04 0.22 ± 0.04 0.011 ± 0.002 0.00 ± 0.00 0.90 ± 0.02 27.12 ± 0.79

0.74 ± 0.08 56.61 ± 3.29 0.91 ± 0.08 0.09 ± 0.08 0.84 ± 0.05 0.14 ± 0.05 0.009 ± 0.001 0.01 ± 0.01 0.94 ± 0.00 23.76 ± 1.31

0.50 ± 0.06 88.69 ± 10.56 0.99 ± 0.01 0.01 ± 0.01 0.83 ± 0.06 0.16 ± 0.06 0.007 ± 0.002 0.00 ± 0.00 0.78 ± 0.04 29.04 ± 2.70

0.68 ± 0.05 63.96 ± 5.60 0.98 ± 0.02 0.02 ± 0.01 0.49 ± 0.23 0.49 ± 0.23 0.006 ± 0.003 0.01 ± 0.01 0.79 ± 0.06 40.46 ± 10.05

0.80 55.32 1.00 0.00 0.81 0.18 0.014 0.00 0.94 24.76

0.82 ± 0.16 53.58 ± 1.06 1.00 0.00 0.52 ± 0.29 0.46 ± 0.29 0.010 ± 0.005 0.00 0.90 ± 0.05 34.29 ± 9.83

0.55 ± 0.00 79.72 ± 0.63 1.00 0.00 0.44 ± 0.17 0.51 ± 0.17 0.006 ± 0.020 0.00 0.65 ± 0.06 49.64 ± 10.78

0.67 ± 0.08 66.35 ± 8.44 0.99 ± 0.02 0.01 ± 0.01 0.47 ± 0.16 0.52 ± 0.17 0.008 ± 0.004 0.01 ± 0.01 0.74 ± 0.11 44.49 ± 11.71

0.48 ± 0.13 96.94 ± 23.19 0.99 ± 0.01 0.01 ± 0.01 0.87 ± 0.03 0.11 ± 0.02 0.014 ± 0.003 0.00 0.80 ± 0.10 27.25 ± 3.93

0.81 ± 0.03 54.13 ± 2.14 1.00 ± 0.00 0.00 0.82 ± 0.11 0.17 ± 0.11 0.010 ± 0.001 0.00 0.95 ± 0.03 24.01 ± 3.70

0.82 ± 0.00 53.52 ± 0.41 1.00 ± 0.00 0.00 0.84 ± 0.03 0.16 ± 0.03 0.008 ± 0.002 0.00 0.95 ± 0.01 23.62 ± 1.17

0.63 69.86 0.97 0.03 0.84 0.14 0.009 0.00 0.86 25.78

0.40 110.02 0.96 0.04 0.89 0.10 0.010 0.00 0.77 27.26

0.75 ± 0.02 59.07 ± 1.48 1.00 ± 0.00 0.00 0.80 ± 0.07 0.19 ± 0.07 0.013 ± 0.001 0.00 0.91 ± 0.02 25.62 ± 2.68

0.72 ± 0.02 60.91 ± 1.60 1.00 ± 0.00 0.00 ± 0.00 0.72 ± 0.07 0.26 ± 0.08 0.013 ± 0.001 0.00 ± 0.00 0.87 ± 0.04 29.53 ± 3.72

0.75 ± 0.05 59.19 ± 3.81 1.00 ± 0.00 0.00 ± 0.00 0.77 ± 0.05 0.21 ± 0.05 0.013 ± 0.002 0.00 ± 0.00 0.90 ± 0.00 26.78 ± 1.20

0.74 ± 0.01 59.42 ± 0.99 1.00 ± 0.00 0.00 ± 0.00 0.81 ± 0.05 0.17 ± 0.05 0.015 ± 0.002 0.00 ± 0.00 0.92 ± 0.02 25.22 ± 1.99

0.72 ± 0.04 60.95 ± 3.33 1.00 ± 0.00 0.00 ± 0.00 0.77 ± 0.16 0.22 ± 0.17 0.013 ± 0.004 0.00 ± 0.00 0.90 ± 0.05 27.36 ± 6.49

0.57 ± 0.12 80.19 ± 17.61 0.95 ± 0.01 0.05 ± 0.01 0.84 ± 0.06 0.14 ± 0.06 0.014 ± 0.001 0.01 ± 0.00 0.85 ± 0.05 26.29 ± 2.72

Carb MVCarb Den Bulk Den Bulk MVCarb XCO2 Carb XCH4 Bulk XH2O Bulk XCO2 Bulk XNaCl Bulk XCH4

304

CO2-CH4

Sample No. Min Stage Min Style Vein Type

Inclusion

type n

133566 1 Mylonite 1 cb 5 -56.6 ± 0.0 0.4 ± 0.1 28.12 ± 1.04 0.65 ± 0.02 67.81 ± 2.50 0.00 ± 0.00 0.64 ± 0.05 69.16 ± 5.47

HBW_1250_12-018 2 Contact qz-cb altn cb 4 -56.7 ± 0.1 0.3 ± 0.1 10.28 ± 3.07 0.86 ± 0.02 51.29 ± 1.33 0.00 ± 0.00 0.85 ± 0.05 51.91 ± 3.48

HBW_1250_12-018 2 Contact qz-cb altn cb 20 -56.6 ± 0.0 0.2 ± 0.1 15.41 ± 4.65 0.81 ± 0.04 54.17 ± 2.73 0.00 ± 0.00 0.81 ± 0.04 54.12 ± 2.57

1213359 2 Fracture 3 cb 2 -57.0 ± 0.2 0.5 ± 0.1 26.25 ± 6.43 0.64 ± 0.16 70.34 ± 16.97 0.01 ± 0.02 0.72 ± 0.03 61.03 ± 3.12

1213359 2 Fracture 3 cb 1 -57.3 0.6 21.20 0.76 57.89 0.01 0.45 97.80

133541 2 Fracture 3 cb 1 -56.6 0.3 20.30 0.77 57.14 0.00 0.82 53.64

133541 2 Fracture 3 cb 2 -56.6 ± 0.0 0.4 ± 0.2 18.40 ± 0.42 0.79 ± 0.00 55.72 ± 0.30 0.00 ± 0.00 0.81 ± 0.00 54.66 ± 0.23

133541 2 Fracture 3 cb 2 -56.6 ± 0.0 0.3 ± 0.0 22.80 ± 1.13 0.74 ± 0.01 59.44 ± 1.16 0.00 ± 0.00 0.77 ± 0.03 57.02 ± 2.35

CH4

Sample No. Min Style Vein No.

1213279 pre-Au Porphyry 2 meth 4 -75.0 ± 1.5

1213279 post-Au Porphyry 2 meth 5 -90.1 ± 0.2

Equiv CO2 Den Equiv CO2 MV

Th Total

Tm CO2 VolFrac Th (L-V) CO2 Density CO2 Molar Volume XCH4

305

H2O-NaCl-(KCl)

Aqueous Gold Related

Sample No Min Stage Min Style Vein type Inclusion Type n

HBW_1250_12-018 2 Contact qz-cb altn aq>>cb 2 -5.7 ± 1.9 0.1 ± 0.0 1.63 ± 0.53 8.65 ± 2.60 0.03 ± 0.01

HBW_1250_12-018 2 Contact qz-cb altn aq>>cb 5 -3.1 ± 2.2 0.1 ± 0.0 0.90 ± 0.65 6.03 ± 2.67 0.02 ± 0.01

HBW_1250_12-018 2 Contact qz-cb altn aq>>cb 7 -2.3 ± 2.0 0.1 ± 0.0 100.5 ± 10.1 0.48 ± 0.48 4.52 ± 3.03 0.01 ± 0.01 0.97 ± 0.01 18.81 ± 0.23

1213359 2 Fracture 3 aq>>cb 5 -3.1 ± 1.8 0.2 ± 0.1 139.9 ± 16.9 160.5 ± 0.7 0.89 ± 0.53 6.85 ± 1.20 0.02 ± 0.01 0.96 ± 0.01 19.42 ± 0.11

Low Salinity Aqueous Post Gold

133566 post-Au Mylonite 1 aq (low sal) 7 -7.6 ± 1.2 0.2 ± 0.3 173.0 ± 29.2 169.1 ± 2.4 2.16 ± 0.34 11.17 ± 1.59 0.04 ± 0.00 0.97 ± 0.02 20.14 ± 0.44

133568 post-Au Mylonite 1 aq (low sal) 11 -7.8 ± 0.9 0.1 ± 0.0 192.0 ± 14.1 2.20 ± 0.24 11.39 ± 1.09 0.04 ± 0.00 0.96 ± 0.02 20.30 ± 0.10

1213279 post-Au Porphyry 2 aq (low sal) 2 -6.4 0.1 1.84 ± 9.71 0.03

1213279 post-Au Porphyry 2 aq (low sal) 5 -5.3 ± 0.8 1.53 ± 0.24 8.22 ± 1.16 0.03 ± 0.00

1213279 post-Au Porphyry 2 aq (low sal) 1 -6.2 1.79 9.45 0.03

1213279 post-Au Porphyry 2 aq (low sal) 1 -7.2 0.1 2.06 10.73 0.04

1213279 post-Au Porphyry 2 aq (low sal) 5 -5.0 ± 2.6 0.1 ± 0.0 1.21 ± 0.80 7.63 ± 3.61 0.02 ± 0.01

1213279 post-Au Porphyry 2 aq (low sal) 2 -2.8 ± 0.8 0.1 ± 0.0 0.82 ± 0.25 4.54 ± 1.32 0.02 ± 0.01



1213279 post-Au Porphyry 2 aq (low sal) 7 -5.7 ± 2.2 233.9 ± 43.5 179.2 ± 17.7 1.41 ± 0.78 6.98 ± 1.09 0.02 ± 0.02 0.85 ± 0.08 22.50 ± 2.05

1213359 post-Au Fracture 3 aq (low sal) 2 -3.3 ± 1.5 0.1 ± 0.0 0.95 ± 0.43 5.21 ± 2.27 0.02 ± 0.01

1213359 post-Au Fracture 3 aq (low sal) 1 -0.7 0.1 0.20 1.16 0.00

1213359 post-Au Fracture 3 aq (low sal) 8 -2.2 ± 1.2 0.1 ± 0.0 117.6 ± 40.6 162.5 ± 2.5 0.63 ± 0.34 3.96 ± 1.57 0.01 ± 0.01 0.97 ± 0.03 19.17 ± 0.70

1213362 post-Au Fracture 3 aq (low sal) 4 -5.8 ± 3.1 0.1 ± 0.0 107.5 ± 51.0 171.3 ± 4.0 2.39 ± 0.69 12.21 ± 3.15 0.04 ± 0.01 1.02 ± 0.03 19.41 ± 0.81

133541 post-Au Fracture 3 aq (low sal) 2 -4.0 ± 1.6





H2O-NaCl-CaCl2

High Salinity Aqueous Post Gold

1213279 post-Au Porphyry 2 aq (high sal) 3 -14.8 ± 0.1 0.1 ± 0.0 3.25 ± 1.06 18.41 ± 0.06 0.06 ± 0.02

HBW_1250_12-018 post-Au Contact qz-cb altn aq (high sal) 11 -19.0 ± 3.1 2.40 ± 0.27 21.02 ± 1.87 0.04 ± 0.00

133541 post-Au Fracture 3 aq (high sal) 6 -21.1 ± 1.7 101.9 ± 22.8 2.59 ± 0.13 22.31 ± 0.89 0.04 ± 0.00 1.16 ± 0.01 19.17 ± 0.12

133541 post-Au Fracture 3 aq (high sal) 9 -19.9 ± 2.3 2.49 ± 0.20 21.63 ± 1.39 0.04 ± 0.00 1.15 ± 0.01 19.14 ± 0.05

1213359 post-Au Fracture 3 aq (high sal) 9 -17.7 ± 1.7 0.1 ± 0.0 89.0 ± 13.5 4.46 ± 0.34 20.66 ± 1.26 0.07 ± 0.01 1.12 ± 0.02 18.72 ± 0.34

X(NaCl) Bulk Den Bulk MVTm ice VolFrac Vap Th L-V ThCREP Molal NaCl Wt% NaCl

306

APPENDICES

307

APPENDIX 5 Laser Raman Analyses

Sample Mineralization Analysis SO2 CO2 CO2 N2 H2S C3H8 CH4 C2H6 NH3 H2 SO2 CO2 N2 H2S C3H8 CH4 C2H6 NH3 H2

Number Style Number 1151 cm-1 1285 cm-1 1388 cm-1 2331 cm-1 2611 cm-1 2899 cm-1 2917 cm-1 2954 cm-1 3334 cm-1 4161 cm-1 mol % mol % mol % mol % mol % mol % mol % mol % mol %

1213279 Porphyry 279_1 1913 3002 619 0 96 0 0 0 4 0 0 01213279 Porphyry 279_2 1767 2919 10497 0 61 0 0 0 39 0 0 01213279 Porphyry 279_3 456 827 0 100 0 0 0 0 0 0 01213279 Porphyry 279_4 300 0 100 0 0 0 0 0 0 01213279 Porphyry 279_5 423 537 0 100 0 0 0 0 0 0 01213279 Porphyry 279_6 378 837 179.5 0 96 0 0 0 4 0 0 01213279 Porphyry 279_7 395 740 137 0 97 0 0 0 3 0 0 01213279 Porphyry 279_8 68.5 392.5 0 100 0 0 0 0 0 0 01213279 Porphyry 279_9 4218 7521.5 1546.5 0 96 0 0 0 4 0 0 01213279 Porphyry 279_10 2196 3965.5 3316 0 86 0 0 0 14 0 0 01213279 Porphyry 279_11 4028 8679 730 0 98 0 0 0 2 0 0 01213279 Porphyry 279_12 650.5 702 0 100 0 0 0 0 0 0 01213279 Porphyry 279_13 734.5 1467 0 100 0 0 0 0 0 0 01213279 Porphyry 279_14 1996.5 2223 0 100 0 0 0 0 0 0 01213279 Porphyry 279_15 11328 0 0 0 0 0 100 0 0 01213279 Porphyry 279_16 15533.5 0 0 0 0 0 100 0 0 01213279 Porphyry 279_17 830 0 0 0 0 0 100 0 0 01213279 Porphyry 279_18 37408.5 0 0 0 0 0 100 0 0 01213279 Porphyry 279_19 55372 0 0 0 0 0 100 0 0 01213279 Porphyry 279_20 318.8 767 68457 1367 0 0 3 0 1 95 1 0 01213279 Porphyry 279_21 26168 0 0 0 0 0 100 0 0 01213279 Porphyry 279_31 13319.5 23900 0 100 0 0 0 0 0 0 0HBW-1250-12-018 Contact 12-18_1 1021.5 3190 0 100 0 0 0 0 0 0 0HBW-1250-12-018 Contact 12-18_2 8065.5 15414 0 100 0 0 0 0 0 0 0HBW-1250-12-018 Contact 12-18_3 3585 6960 0 100 0 0 0 0 0 0 0HBW-1250-12-018 Contact 12-18_4 1559 2990 0 100 0 0 0 0 0 0 0HBW-1250-12-018 Contact 12-18_5 758.5 939 0 100 0 0 0 0 0 0 0HBW-1250-12-018 Contact 12-18_6 246 418.5 0 100 0 0 0 0 0 0 0133541 Fracture 541_1 305.5 654.5 0 100 0 0 0 0 0 0 0133541 Fracture 541_2 3206 5460 0 100 0 0 0 0 0 0 0133541 Fracture 541_3 545 733 0 100 0 0 0 0 0 0 0133541 Fracture 541_4 105 1851 0 100 0 0 0 0 0 0 0133541 Fracture 541_5 12034.5 24037 0 100 0 0 0 0 0 0 0133541 Fracture 541_6 8402.5 15704 0 100 0 0 0 0 0 0 0133541 Fracture 541_7 4911 9759.5 0 100 0 0 0 0 0 0 0133541 Fracture 541_8 4526 9563 0 100 0 0 0 0 0 0 0133541 Fracture 541_9 2246 4953 0 100 0 0 0 0 0 0 0133541 Fracture 541_10 10437 20670.5 0 100 0 0 0 0 0 0 0133541 Fracture 541_11 25450.5 49492 0 100 0 0 0 0 0 0 0133541 Fracture 541_12 929 1991.5 0 100 0 0 0 0 0 0 0133541 Fracture 541_13 4137 7583 0 100 0 0 0 0 0 0 0133541 Fracture 541_14 9474 16197 0 100 0 0 0 0 0 0 0

308

APPENDICES

309

APPENDIX 6 LA-ICP-MS Fluid Inclusion Analyses

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt %

NaCl

Mg/Na K/Na Cu/Na Zn/Na As/Na Sr/Na Ag/Na Ba/Na Pb/Na

1213279 I 2 aq-cb 3.05 0.028097 0.0007091213279 I 2 aq-cb 3.05 0.102929 0.194728 0.042546 0.000531 0.0005971213279 I 2 aq-cb 3.05 0.261015 0.071338 0.004984 0.000139 0.006633 0.0002451213279 I 2 aq-cb 3.05 0.128909 0.059892 0.0158901213279 I 2 aq-cb 3.05 0.0069431213279 I 2 aq-cb 3.05 0.202924 0.008094 0.003840 0.000246 0.000108 0.001913 0.0004891213279 I 2 aq-cb 3.05 0.149608 0.000225 0.000893 0.0031571213279 I 2 aq-cb 3.05 0.000526 0.001682 0.0004501213279 I 2 aq-cb 3.05 0.0350081213279 I 2 aq-cb 3.05 0.053482 0.069080 0.029639 0.000720 0.000368 0.002955 0.0009071213279 I 2 aq-cb 3.05 0.096602 0.028783 0.007310 0.000194 0.011923 0.0009571213279 I 2 aq-cb 3.05 0.069243 0.019671 0.000726 0.000140 0.0011931213279 I 2 aq-cb 3.05 0.007201 0.001668 0.000634 0.001317 0.0003761213279 I 2 aq-cb 3.05 0.007843 0.000586 0.002283 0.0007251213279 I 2 aq-cb 3.05 0.233990 0.130006 0.007989 0.001552 0.000305 0.0005491213279 I 2 aq-cb 3.05 0.014218 0.000163 0.0003031213279 I 2 aq-cb 3.05 0.005942 0.001558 0.000571 0.002156 0.0004111213279 I 2 aq-cb 3.05 0.098652 0.321233 0.0006871213279 I 2 aq-cb 3.051213279 I 2 aq-cb 3.05 0.361304 0.053635 0.009867 0.004415 0.000813 0.0014671213279 I 2 aq-cb 3.05 0.382257 0.006977 0.000551 0.0067811213279 I 2 aq-cb 3.05 0.151359 0.006897 0.001970 0.005719 0.0004021213279 I 2 aq-cb 3.05 0.406243 0.044501 0.0214931213279 I 2 aq-cb 3.05 0.394739 0.048872 0.0020811213279 I 2 aq-cb 3.05 0.002042 0.0013001213279 I 2 aq-cb 3.05 0.391012 0.071021 0.046828 0.006899 0.003725 0.0002851213279 I 2 aq-cb 3.05 0.249105 0.454627 0.022430 0.001105 0.000476 0.0034261213279 I 2 aq-cb 3.05 0.554715 0.0002371213279 I 2 aq-cb 3.05 0.356242 0.133949 0.053923 0.005757 0.018537 0.000441 0.0015221213279 I 2 aq-cb 3.05 0.013133 0.004571 0.010588 0.000209 0.0041721213279 I 2 aq-cb 3.05 0.265913 0.246106 0.013190 0.015190 0.002734 0.0016871213279 I 2 aq-cb 3.05 0.312217 0.171426 0.031619 0.010254 0.000571 0.0020411213279 I 2 aq-cb 3.05 0.100857 0.329980 0.014443 0.002545 0.000412 0.0029171213279 I 2 aq-cb 3.05 0.233837 0.224473 0.016104 0.028755 0.004406 0.001058 0.0041581213279 I 2 aq-cb 3.05 0.077791 0.478202 0.0006111213279 I 2 aq-cb 3.05 0.445825 0.042267 0.000287 0.0010661213279 I 2 aq-cb 3.05 0.227009 0.025295 0.004710 0.000293 0.0012731213279 I 2 aq-cb 3.05 0.079839 0.434813 0.023545 0.000571 0.000813 0.0034391213279 I 2 aq-cb 3.051213279 I 2 aq-cb 3.051213279 I 2 aq-cb 3.05 0.0090061213279 I 2 aq-cb 3.05 0.100243 0.000813 0.000212 0.001890 0.0004111213279 I 2 aq-cb 3.05 0.440472 0.006091 0.0124831213279 I 2 aq-cb 3.05 0.108768 0.517036 0.003044 0.000599 0.000462

310

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt %

NaCl


1213279 I 2 aq-cb 3.05 0.009728 0.010527 0.014240 0.001100 0.000988 0.003242 0.0006061213279 I 2 aq-cb 3.05 0.006323 0.001156 0.000174 0.000729 0.000222

mean mean 0.196370 0.285434 0.027988 0.012759 0.007392 0.000800 0.000570 0.003117 0.000473sd std 0.113085 0.159983 0.017987 0.008617 0.005021 0.000567 0.000363 0.002404 0.000219

HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.376052 0.119208 0.004549 0.013702 0.016377 0.009298 0.003518HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.453540 0.042650 0.004482 0.004192 0.012480 0.003640HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.498685 0.087033 0.017580 0.028317 0.012803HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.038257 0.001909 0.001548 0.000312 0.000870 0.001244HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.026811 0.003025 0.005677HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.001704 0.003971HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.015054 0.000107 0.014382 0.002736HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.010942 0.004680 0.004317HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.044463 0.002195 0.000432

mean 0.442759 0.066322 0.007893 0.012692 0.014179 0.006733 0.000107 0.006574 0.003577sd 0.062023 0.035538 0.006359 0.010406 0.017864 0.006866 0.005318 0.001501

133541 II 3 aq-cb 5.12 0.545632 0.154956 0.011480 0.0077798 0.00027435 0.00680335 0.0226979133541 II 3 aq-cb 5.12 0.402562 0.217582 0.0364819 0.00919391 0.0275794133541 II 3 aq-cb 5.12 0.030349 0.0356152133541 II 3 aq-cb 5.12 0.0134266 0.173106 0.0178273 0.00081208 0.0001447133541 II 3 aq-cb 5.12 0.039565 0.0014642 0.00041007 0.00733956 0.0051342133541 II 3 aq-cb 5.12 0.0133936 0.427411 0.021287 0.0374716 0.00027054 0.0064742133541 II 3 aq-cb 5.12 0.120121 0.0165723 0.020449 0.00658373133541 II 3 aq-cb 5.12 0.0105081 0.319133 0.003312 0.0001799 0.00010031 0.00147006133541 II 3 aq-cb 5.12 0.028735 0.373304 0.0132996 0.003113 0.0056442 0.00128508133541 II 3 aq-cb 5.12133541 II 3 aq-cb 5.12 0.0915088 0.345131 0.0275483 0.00072671 0.0171841133541 II 3 aq-cb 5.12 0.345663 0.0418282 0.00013986133541 II 3 aq-cb 5.12 0.00873945 0.0151756133541 II 3 aq-cb 5.12 0.0331078 0.293209 0.0128993 0.00107564 0.0009604 0.0013021133541 II 3 aq-cb 5.12 0.0349565 0.287033 0.0113253 0.00124021 0.00126753 0.00153409 0.003317133541 II 3 aq-cb 5.12 0.356895 0.00806261 0.00780692 0.00210429 0.00045382 0.0060738133541 II 3 aq-cb 5.12 0.313118 0.00031533133541 II 3 aq-cb 5.12 0.546902 0.437486 0.00153734 0.00271499 0.0084969133541 II 3 aq-cb 5.12 0.465074 0.0012834 0.0147297

mean 0.188875 0.305166 0.020711 0.016534 0.018691 0.000984 0.000681 0.004618 0.012686sd 0.2249048 0.10689627 0.01228716 0.01377576 0.01447496 0.0006337 0.00054146 0.003185287 0.0081467

1213359 II 3 aq (low sal) 8.36 0.00731515 0.00255891 0.000709447 0.0107844

311

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt %

NaCl


1213359 II 3 aq (low sal) 8.36 0.1329941213359 II 3 aq (low sal) 8.36 0.0685528 0.270384 0.010582 0.000687251213359 II 3 aq (low sal) 8.36 0.0798921 0.3924 0.00644777 0.00946374 0.00103713 0.000595 0.00196211213359 II 3 aq (low sal) 8.36 0.272685 0.00163653 0.005596 0.0224773 0.00092989 0.00259431213359 II 3 aq (low sal) 8.36 0.0501835 0.209951 0.00592022 0.009226 0.00227697 0.00208971213359 II 3 aq (low sal) 8.36 0.272014 0.002971 0.0143143 0.000240871213359 II 3 aq (low sal) 8.36 0.00837466 0.0141742 0.00366726 0.000878225 0.00154891213359 II 3 aq (low sal) 8.36 0.0237979 0.484319 0.00813597 0.008389 0.00094207 0.00064816 0.00181437 0.00672311213359 II 3 aq (low sal) 8.36 0.0399475 0.232845 0.011101 0.016299 0.00398419 0.0037135 0.001655451213359 II 3 aq (low sal) 8.36 0.077152 0.426661 0.00462747 0.015170 0.000467181213359 II 3 aq (low sal) 8.36 0.0129497 0.261816 0.00103492 0.00352161213359 II 3 aq (low sal) 8.36 0.232947 0.00246622 0.000446671213359 II 3 aq (low sal) 8.36 0.0127851 0.465794 0.00318029 0.004744 0.00031976 0.000482106 0.00635041213359 II 3 aq (low sal) 8.36 0.20771 0.003456 0.00204146 0.0017976

mean 0.0456576 0.29711692 0.0063443 0.00823124 0.01089263 0.00224911 0.00052734 0.001278663 0.0044263sd 0.10928612 0.00314978 0.00512447 0.00781618 0.00139673 0.00013997 0.000589259 0.0032563

133541 Post Au 3 aq (high sal) 20.60 0.0116738 0.669757 0.00423093 8.44E-05 0.00045464 0.000509804 0.0006023133541 Post Au 3 aq (high sal) 20.60 0.0066753 0.551605 0.00416912 0.00012706 0.00018708 0.0007023133541 Post Au 3 aq (high sal) 20.60 0.0134009 0.605239 0.00016667 0.000272639133541 Post Au 3 aq (high sal) 20.60 0.642002 0.0037855 0.00191329 0.000337524 0.0007702133541 Post Au 3 aq (high sal) 20.60 0.0128196 0.576761 0.00484161 0.00012336 0.00252964 0.00038539 0.0001235133541 Post Au 3 aq (high sal) 20.60 0.0122512 0.66139 0.00176193 9.11E-05 0.0003028133541 Post Au 3 aq (high sal) 20.60 0.0096019 0.00296798 0.000287 9.81E-05 0.00073218 0.0004009133541 Post Au 3 aq (high sal) 20.60 0.0078167 0.00287035 0.000956 7.25E-05 0.00301395 0.000120544 0.0003849133541 Post Au 3 aq (high sal) 20.60 0.0075319 0.00235274 0.00013507 0.00177072 0.0002238133541 Post Au 3 aq (high sal) 20.60 0.0069164 0.58278 0.00332403 9.83E-05 0.0003594133541 Post Au 3 aq (high sal) 20.60 0.0036667 0.823269 0.00251524 7.55E-05133541 Post Au 3 aq (high sal) 20.60 0.0071198 0.856597 0.001822 0.00215617 0.0002558133541 Post Au 3 aq (high sal) 20.60 0.552908 0.00225278 1.83E-05133541 Post Au 3 aq (high sal) 20.60 0.0060826 0.622222 0.00754104 0.00013485 0.0002701

mean 0.64950273 0.0035511 0.00102157 0.00010211 0.0017958 0.000302164 0.0003996sd 0.10249481 0.00155899 0.00076999 3.8701E-05 0.00092166 0.000140281 0.0002063

HBW_1250_12-018 Post Au qz-cb altn aq (high sal) 21.00 0.028771 0.050000 0.001053 0.000145 0.000828 0.000018 0.001252 0.001566HBW_1250_12-018 Post Au qz-cb altn aq (high sal) 21.00 0.021329 0.391930 0.000751 0.013576 0.005051HBW_1250_12-018 Post Au qz-cb altn aq (high sal) 21.00 0.050000 0.003389 0.000406 0.004822HBW_1250_12-018 Post Au qz-cb altn aq (high sal) 21.00 0.069384 0.453569 0.012583 0.000189 0.000676 0.001096

mean 0.0150027 0.52011921 0.00380874 0.00083351 0.00016403 0.00139438 0.001991437 0.0007947sd 0.21667324 0.00609534 0.00032482 0.00040317 0.006340856 0.0021606

312

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl

Ca/Na Mn/Na Fe/Na Mo/Na Sn/Na Cs/Na W/Na Th/Na U/Na

1213279 I 2 aq-cb 3.05 0.280817 0.000453 0.0002266 0.0001353

1213279 I 2 aq-cb 3.05 0.452375 0.000202 0.001327

1213279 I 2 aq-cb 3.05 0.874771 0.021779 0.0005572

1213279 I 2 aq-cb 3.05 0.060310 0.003007 0.0004472

1213279 I 2 aq-cb 3.05 0.596489

1213279 I 2 aq-cb 3.05 0.014312 0.001161 0.0003291

1213279 I 2 aq-cb 3.05 0.004796 0.037043 0.0001459 0.0000351 0.0005316

1213279 I 2 aq-cb 3.05 0.002295 0.0003262 0.0005096

1213279 I 2 aq-cb 3.05 0.007439 0.011083 0.0011115

1213279 I 2 aq-cb 3.05 0.000756 0.0002405

1213279 I 2 aq-cb 3.05 0.002938 0.028199 0.0000130 0.0008503

1213279 I 2 aq-cb 3.05 0.003959 0.001415 0.0001947 0.0020055 0.0007981

1213279 I 2 aq-cb 3.05 0.001830 0.0004560

1213279 I 2 aq-cb 3.05 0.0003719 0.0020432 0.0006098

1213279 I 2 aq-cb 3.05

1213279 I 2 aq-cb 3.05 0.032000 0.000524 0.000919 0.0000410 0.0001374

1213279 I 2 aq-cb 3.05 0.022451 0.0000539 0.0001089 0.0000161

1213279 I 2 aq-cb 3.05 0.056738 0.004780 0.0000746 0.0005909 0.0001745

1213279 I 2 aq-cb 3.05 0.072320 0.000658 0.002117 0.0007289 0.0002870

1213279 I 2 aq-cb 3.05 0.058473 0.001390 0.0003088 0.0001823

1213279 I 2 aq-cb 3.05 0.202766 0.063975 0.000785 0.003677 0.0000826 0.0006113 0.0003610

1213279 I 2 aq-cb 3.05 0.000623 0.002963 0.0004424 0.0001408

1213279 I 2 aq-cb 3.05 0.002125 0.0000360 0.0003555

1213279 I 2 aq-cb 3.05 0.006342 0.007162 0.0007913

1213279 I 2 aq-cb 3.05 0.0014680 0.0017526

1213279 I 2 aq-cb 3.05 0.065712 0.004488 0.0002902

1213279 I 2 aq-cb 3.05

1213279 I 2 aq-cb 3.05 0.006145 0.0004289 0.0002533 0.0002560

1213279 I 2 aq-cb 3.05 0.004445 0.0011669 0.0004644

mean 0.481444 0.004783 0.039338 0.000994 0.003409 0.0001685 0.0008070 0.0002043 0.0006419

sd 0.26772145 0.00192676 0.0228528 0.00064935 0.0019371 0.0001461 0.0006564 0.0001379 0.0004152

HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.015691 0.000000 0.0254157

HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.023103 0.000262 0.000543 0.0000344 0.0337053 0.0004918


HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.084938 0.002458 0.037214 0.001358 0.003506 0.0645274 0.0004245



HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.009255 0.005236

313

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl




HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.058091 0.026455 0.001973 0.0004649 0.0783873


HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.006964 0.001091 0.0005970 0.0002645





HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.008560 0.000277 0.001158 0.0000653

HBW_1250_12-018 II qz-cb altn aq-cb 4.51

mean 0.068566 0.004685 0.069809 0.000674 0.002425 0.0002710 0.0368925 0.0003982 0.0003726

sd 0.057619 0.003377 0.045852 0.000608 0.001694 0.0002408 0.0235335 0.0002892 0.0002416

133541 II 3 aq-cb 5.12 0.0990294 0.001868 0.0011282 0.0002964 0.0003962 0.0001913 0.0000206

133541 II 3 aq-cb 5.12 0.001849 0.001088 0.0000710

133541 II 3 aq-cb 5.12 0.0100082 0.000282 0.0038374 0.0001916 0.0008292 0.0002002

133541 II 3 aq-cb 5.12 0.0584911 0.0070988 0.000487 0.0025146 0.0002324

133541 II 3 aq-cb 5.12 0.0025382 0.0000226 0.0000125

133541 II 3 aq-cb 5.12 0.0164192 0.0007149 0.0001100 0.0000626 0.0000080

133541 II 3 aq-cb 5.12 0.0000121 0.0000154

133541 II 3 aq-cb 5.12

mean 0.057980 0.010008 0.003451 0.001121 0.002142 0.0001979 0.0003369 0.0001191 0.0000141

sd 0.04130747 0.0032883 0.0008552 0.0013104 0.0000949 0.0003664 0.0000900 0.0000053

1213359 II 3 aq-cb 3.80 Ca/Na Mn/Na Fe/Na Mo/Na Sn/Na Cs/Na W/Na Th/Na U/Na

1213359 II 3 aq-cb 3.80 0.00038793

1213359 II 3 aq-cb 3.80 0.00117054 0.0932153 0.0037815 0.0007929 0.0001827 0.0000356

1213359 II 3 aq-cb 3.80 0.000049 0.003165 0.0002002 0.0003994 0.0003321

1213359 II 3 aq-cb 3.80 0.0733388 0.00065081 0.0003809

1213359 II 3 aq-cb 3.80 0.255204 0.00053937 0.0001887

1213359 II 3 aq-cb 3.80 0.29341 0.0587841 0.0031206 0.0002218

1213359 II 3 aq-cb 3.80 0.194552 0.000208 0.0040372 0.0003016 0.0000838

1213359 II 3 aq-cb 3.80 0.0882645 0.000211 0.0015792

1213359 II 3 aq-cb 3.80 0.132954 0.0435538 0.000163

1213359 II 3 aq-cb 3.80 0.078106 0.0611506 0.0011314 0.0000588 0.0003520 0.0001153

1213359 II 3 aq-cb 3.80 0.0018754 0.0002531 0.0000622

314

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl


1213359 II 3 aq-cb 3.80 0.0674895 0.0001321 0.0005181 0.0007504 0.0002545

1213359 II 3 aq-cb 3.80 0.0296443 0.0034049 0.0001937 0.0008074

1213359 II 3 aq-cb 3.80 0.0651259 0.0049634 0.0002966 0.0002923 0.0002974

mean 0.14502253 0.00068716 0.0624354 0.00015781 0.0030065 0.0001703 0.0004446 0.0003613 0.0001687

sd 0.09162722 0.00033978 0.0247439 7.579E-05 0.0012511 0.0001007 0.0002673 0.0001884 0.0001223

133541 Post Au 3 aq (high sal) 20.60 0.082907 0.00307254 0.0044006 0.0013331 0.0001523

133541 Post Au 3 aq (high sal) 20.60 0.00025941

133541 Post Au 3 aq (high sal) 20.60 0.00247188 0.0019496 0.0001441

133541 Post Au 3 aq (high sal) 20.60 0.00150794 0.0000399 0.0001254 0.0001497

133541 Post Au 3 aq (high sal) 20.60 0.15013 0.00113061 0.0024231 0.0009379 0.0000695 0.0001036 0.0000618



133541 Post Au 3 aq (high sal) 20.60 0.0751084 0.0000122


mean 0.10902357 0.00136137 0.0034005 0.0009897 0.0000286 0.0000735 0.0001270

sd 0.02721852 0.00106366 0.0012035 0.0006982 0.0000226 0.0000485 0.0000436

315

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl

K/Na Sb/Na Au/Na Bi/Na

1213279 I 2 aq-cb 3.05 0.278518 0.000172

1213279 I 2 aq-cb 3.05 0.004612

1213279 I 2 aq-cb 3.05 0.111925 0.007725

1213279 I 2 aq-cb 3.05 0.279323 0.001279

1213279 I 2 aq-cb 3.05 0.001384

1213279 I 2 aq-cb 3.05 0.000269

1213279 I 2 aq-cb 3.05 0.164287

1213279 I 2 aq-cb 3.05 0.006813

1213279 I 2 aq-cb 3.05 0.255672 0.000372 0.000409

1213279 I 2 aq-cb 3.05 0.002746

1213279 I 2 aq-cb 3.05

1213279 I 2 aq-cb 3.05 0.217235 0.000695

1213279 I 2 aq-cb 3.05

1213279 I 2 aq-cb 3.05 0.329263 0.000157

1213279 I 2 aq-cb 3.05 0.429522 0.001129 0.000293

1213279 I 2 aq-cb 3.05 0.168506 0.000031

1213279 I 2 aq-cb 3.05 0.142331 0.000017

1213279 I 2 aq-cb 3.05 0.164718 0.000178

1213279 I 2 aq-cb 3.05 0.433613 0.002946 0.000131

1213279 I 2 aq-cb 3.05 0.162481 0.003100 0.000067

1213279 I 2 aq-cb 3.05 0.002911

1213279 I 2 aq-cb 3.05 0.000018

1213279 I 2 aq-cb 3.05 0.000015 0.000221

1213279 I 2 aq-cb 3.05 0.000682

1213279 I 2 aq-cb 3.05 0.001648 0.000062 0.001551

1213279 I 2 aq-cb 3.05 0.125240 0.003467 0.000083 0.000733

1213279 I 2 aq-cb 3.05 0.303507 0.000193

1213279 I 2 aq-cb 3.05 0.000397

1213279 I 2 aq-cb 3.05 0.348050 0.002471 0.000604

1213279 I 2 aq-cb 3.05 0.000456 0.000211

1213279 I 2 aq-cb 3.05 0.001174

1213279 I 2 aq-cb 3.05 0.351870 0.002274 0.000075 0.002218

1213279 I 2 aq-cb 3.05 0.007071 0.000183 0.002446

1213279 I 2 aq-cb 3.05

mean 0.250945 0.003438 0.000161 0.001128

sd 0.103979 0.002288 0.000137 0.000882

HBW_1250_12-018 II qz-cb altn aq-cb 4.51 0.456242



























316

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl

K/Na Sb/Na Au/Na Bi/Na




mean 0.518711 0.003736 0.000107 0.003559

sd 0.118118 0.003204 0.000155 0.003499

133541 II 3 aq-cb 5.12 0.579152

133541 II 3 aq-cb 5.12 1.011990

133541 II 3 aq-cb 5.12 0.941967 0.029460

133541 II 3 aq-cb 5.12 0.003525

133541 II 3 aq-cb 5.12 1.038910 0.007405 0.000027

133541 II 3 aq-cb 5.12 1.044640 0.000024 0.002494

133541 II 3 aq-cb 5.12 1.005950 0.005976

133541 II 3 aq-cb 5.12 0.582590 0.013796

mean 0.886457 0.014280 0.000026 0.006605

sd 0.211406 0.013165 0.000002 0.006249

1213359 II 3 aq-cb 3.8 0.637667

1213359 II 3 aq-cb 3.8 0.522013 0.00086214 0.005965

1213359 II 3 aq-cb 3.8 2.45E-05

1213359 II 3 aq-cb 3.8 0.691976

1213359 II 3 aq-cb 3.8 8.59E-06

1213359 II 3 aq-cb 3.8 0.510229 0.003296

1213359 II 3 aq-cb 3.8 0.554747

1213359 II 3 aq-cb 3.8 0.696581

1213359 II 3 aq-cb 3.8 0.489834

1213359 II 3 aq-cb 3.8 0.269164 0.000179

1213359 II 3 aq-cb 3.8 0.766514 0.0025796

1213359 II 3 aq-cb 3.8 0.00564176 0.0002209

1213359 II 3 aq-cb 3.8 0.560313

1213359 II 3 aq-cb 3.8 0.560313

1213359 II 3 aq-cb 3.8 0.755917 0.00470082 0.002826

1213359 II 3 aq-cb 3.8 3.11E-06

1213359 II 3 aq-cb 3.8 0.842841 0.0053513 7.32E-05 0.000586

1213359 II 3 aq-cb 3.8 0.581059 0.0023535

1213359 II 3 aq-cb 3.8 0.475053 0.00377486 8.53E-06 0.000335

1213359 II 3 aq-cb 3.8 0.474423

1213359 II 3 aq-cb 3.8 0.444057

1213359 II 3 aq-cb 3.8

1213359 II 3 aq-cb 3.8 0.320623 0.00291294

1213359 II 3 aq-cb 3.8

1213359 II 3 aq-cb 3.8 0.603475 0.00238599

1213359 II 3 aq-cb 3.8 0.460853 0.000400

mean 0.5608826 0.00339588 7.398E-05 0.00223451

sd 0.14400716 0.00158666 9.005E-05 0.00223999










mean 0.582803 0.000174 0.000034 0.000202

sd 0.379794 0.000053 0.000034 0.000305

317

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl

Au/Na

1213279 I 2 aq-cb 3.05 0.001927

1213279 I 2 aq-cb 3.05 0.001799

1213279 I 2 aq-cb 3.05 0.000384

1213279 I 2 aq-cb 3.05 0.000444

1213279 I 2 aq-cb 3.05 0.000145

1213279 I 2 aq-cb 3.05 0.000180

1213279 I 2 aq-cb 3.05 0.000287

1213279 I 2 aq-cb 3.05 0.000073

1213279 I 2 aq-cb 3.05 0.000721

1213279 I 2 aq-cb 3.05 0.000381

1213279 I 2 aq-cb 3.05 0.000416

1213279 I 2 aq-cb 3.05 0.000139

1213279 I 2 aq-cb 3.05 0.000111

1213279 I 2 aq-cb 3.05 0.001554

1213279 I 2 aq-cb 3.05 0.000716

1213279 I 2 aq-cb 3.05 0.000276

1213279 I 2 aq-cb 3.05 0.000458

1213279 I 2 aq-cb 3.05 0.008821

1213279 I 2 aq-cb 3.05 0.002366

1213279 I 2 aq-cb 3.05 0.000092

1213279 I 2 aq-cb 3.05 0.000530

1213279 I 2 aq-cb 3.05 0.001004

1213279 I 2 aq-cb 3.05 0.001262

1213279 I 2 aq-cb 3.05 0.001062

1213279 I 2 aq-cb 3.05 0.000452

1213279 I 2 aq-cb 3.05 0.000280

1213279 I 2 aq-cb 3.05 0.002712

1213279 I 2 aq-cb 3.05 0.000422

1213279 I 2 aq-cb 3.05 0.004642

1213279 I 2 aq-cb 3.05 0.000108

1213279 I 2 aq-cb 3.05 0.000888

1213279 I 2 aq-cb 3.05 0.000560

1213279 I 2 aq-cb 3.05 0.000097

1213279 I 2 aq-cb 3.05 0.000135

1213279 I 2 aq-cb 3.05 0.000026

1213279 I 2 aq-cb 3.05 0.000043

1213279 I 2 aq-cb 3.05 0.000607

1213279 I 2 aq-cb 3.05 0.000542

1213279 I 2 aq-cb 3.05 0.000221

1213279 I 2 aq-cb 3.05 0.000111

1213279 I 2 aq-cb 3.05 0.003680

1213279 I 2 aq-cb 3.05 0.006658

1213279 I 2 aq-cb 3.05 0.000040

1213279 I 2 aq-cb 3.05 0.000308

1213279 I 2 aq-cb 3.05 0.000172

1213279 I 2 aq-cb 3.05 0.000372

1213279 I 2 aq-cb 3.05 0.000157

1213279 I 2 aq-cb 3.05 0.000293

1213279 I 2 aq-cb 3.05 0.000031

1213279 I 2 aq-cb 3.05 0.000017

1213279 I 2 aq-cb 3.05 0.000178

1213279 I 2 aq-cb 3.05 0.000131

1213279 I 2 aq-cb 3.05 0.000067

1213279 I 2 aq-cb 3.05 0.000018

1213279 I 2 aq-cb 3.05 0.000015

1213279 I 2 aq-cb 3.05 0.000062

1213279 I 2 aq-cb 3.05 0.000083

1213279 I 2 aq-cb 3.05 0.000193

1213279 I 2 aq-cb 3.05 0.000397

1213279 I 2 aq-cb 3.05 0.000456

1213279 I 2 aq-cb 3.05 0.000075

1213279 I 2 aq-cb 3.05 0.000183

mean 0.000816

sd 0.0015559






318

Sample NoMin

StageVein Type

Inclusion

Type

Salinity

(equiv. wt

% NaCl

Au/Na

















mean 0.000748

sd 0.0011358

133541 II 3 aq-cb 5.12 0.001537

133541 II 3 aq-cb 5.12 0.001607

133541 II 3 aq-cb 5.12 0.000320

133541 II 3 aq-cb 5.12 0.001109

133541 II 3 aq-cb 5.12 0.000280

133541 II 3 aq-cb 5.12 0.000198

133541 II 3 aq-cb 5.12 0.000005

133541 II 3 aq-cb 5.12 0.000157

133541 II 3 aq-cb 5.12 0.000019

133541 II 3 aq-cb 5.12 0.000575

133541 II 3 aq-cb 5.12 0.001326

133541 II 3 aq-cb 5.12 0.000033

133541 II 3 aq-cb 5.12 0.000128

133541 II 3 aq-cb 5.12 0.000330

133541 II 3 aq-cb 5.12 0.000028

133541 II 3 aq-cb 5.12 0.001407

133541 II 3 aq-cb 5.12 0.000023

133541 II 3 aq-cb 5.12 0.000067

133541 II 3 aq-cb 5.12 0.000081

mean 0.0004858

sd 0.0005843

1213359 II 3 aq-cb 3.8 0.000118

1213359 II 3 aq-cb 3.8 0.000509

1213359 II 3 aq-cb 3.8 0.001193

1213359 II 3 aq-cb 3.8 0.000213

1213359 II 3 aq-cb 3.8 0.000270

1213359 II 3 aq-cb 3.8 0.000117

1213359 II 3 aq-cb 3.8 0.000118

1213359 II 3 aq-cb 3.8 0.000083

1213359 II 3 aq-cb 3.8 0.002107

1213359 II 3 aq-cb 3.8 0.001450

1213359 II 3 aq-cb 3.8 0.000083

1213359 II 3 aq-cb 3.8 0.000122

1213359 II 3 aq-cb 3.8 0.002151

1213359 II 3 aq-cb 3.8 0.000187

1213359 II 3 aq-cb 3.8 0.001944

1213359 II 3 aq-cb 3.8 0.000822

1213359 II 3 aq-cb 3.8 0.000079

1213359 II 3 aq-cb 3.8 0.000105

1213359 II 3 aq-cb 3.8 0.002386

1213359 II 3 aq-cb 3.8 0.000091

1213359 II 3 aq-cb 3.8 0.000185

mean 0.000587

sd 0.0006991

319

APPENDICES

320

APPENDIX 7 Sulfur Isotopic Analyses

Sample No Deposit/Camp Mineralising Event

Mineralisation Style

Sample DescriptionPyrite Description Method δ34S (‰)

Analytical precision

Reference

1213279 New Celebration Stage I Porphyry

M1 carbonate altered plagioclase porphyry Anhedral, sheared,

located in S3NC

foliation planesBulk -2.41 This study

133543 New Celebration Stage I PorphyryM1 carbonate altered plagioclase porphyry

S3NC-related anhedral, coarse-grained

Bulk -3.29 This study


S3NC-related anhedral, coarse-grained


1213279 New Celebration Stage I PorphyryM1 carbonate altered plagioclase porphyry Anhedral, grains

intergrown, 1000μmLA -4.14 0.006 This study


Anhedral, several grains in foliation plane, 300μm

LA -5.72 0.005 This study


M1 carbonate altered plagioclase porphyry Anhedral, elongate,

located in foliation plane, 500μm






Anhedral, disseminated, 250μm






M1 carbonate altered plagioclase porphyry Subhedral-euhedral,

disseminated, 100-200μm



M1 carbonate altered plagioclase porphyry Fine-grained,

anhedral, located in S3NC foliation planes


1213226 New Celebration Stage I Mylonite

Quartz-carbonate mylonite

Anhedral, sheared, located in S3NC

foliation planes, 400μm

Bulk 2.03 This study


Quartz-carbonate mylonite

Anhedral, sheared, located in S3NC

foliation planes, 400μm

LA 3.77 0.220 This study


Quartz-carbonate mylonite Anhedral, aligned

along S3NC foliation planes, 200μm


















1213371 New Celebration Stage II Contact

Quartz-carbonate-fuchsite-altered contact between M2 quartz-feldspar porphyry and high-Mg basalt

Subhedral, disseminated, 800μm

Bulk 1.14 This study



Semi-massive, anhedral grains, aligned along S3NC

foliation planes at contact, 400-1000μm


321





Reference


























1250_12-018 New Celebration Stage II Contact




















1149198 New Celebration Stage II Fracture

M2 albite-carbonate altered quartz-feldspar phyric porphyry

Coarse-grained, euhedral




Coarse-grained, euhedral




Coarse-grained, subhedral to euhedral, zoned




Coarse-grained, subhedral to euhedral.




Anhedral, 200-500μm






322





Reference

















121763 New CelebrationSericite-altered sheared porphyritic intrusion Subhedral, 100μm LA -1.41 0.12 Hodkiewicz,

2003

121766 New CelebrationBiotite-dolomite-chlorite-altered ultramific schist Subhedral, 100μm LA 3.92 0.015 Hodkiewicz,

2003

121776 New CelebrationChlorite-calcite-albite-altered mafic schist Euhedral, 300μm LA 5.54 0.038 Hodkiewicz,

2003

121784 New CelebrationAlbite-hematite-altered sheared felsic porphyry Euhedral, 800μm LA -8.64 0.032 Hodkiewicz,

2003

121784 New CelebrationAlbite-hematite-altered sheared felsic porphyry Euhedral, 300μm LA -6.78 0.026 Hodkiewicz,

2003

121784 New CelebrationAlbite-hematite-altered sheared felsic porphyry Subhedral, 500μm LA -6.04 0.012 Hodkiewicz,

2003

121788 New CelebrationK-feldspar-albite-ankerite-altered tholeiitic mafic schist

Euhedral, 500μm LA -4.84 0.046 Hodkiewicz, 2003

121788 New CelebrationK-feldspar-albite-ankerite-altered tholeiitic mafic schist

Euhedral, 1000μm LA -5.49 0.016 Hodkiewicz, 2003

LG106 Golden Mile Synvolcanic sulfide

Chlorite altered Paringa Basalt

Coarse-grained, anhedral massive


LG106 Golden Mile Synvolcanic sulfide

Chlorite altered Paringa Basalt

Coarse-grained, anhedral massive


UG1

Golden Mile Fimiston Stage IQuartz-carbonate-chlorite altered Golden Mile Dolerite (U8)

Medium-grained, subhedral, glomerocrystic grains, 500µm


UG1

Golden Mile Fimiston Stage IQuartz-carbonate-chlorite altered Golden Mile Dolerite (U8)

Fine-grained, subhedral, glomerocrystic grains, 300µm


233

Golden Mile Fimiston Stage II

Foliated carbonate-albite±quartz altered mafic dyke in Golden Mile Dolerite

Fine-grained, euhedral pyrite, 300µm


233



Very fine-grained pyrite glomerocrysts, 20µm


233





233





52280

Golden Mile Fimiston Stage IIPyrite-tourmaline vein in Golden Mile Dolerite (U8)

Coarse-grained, anhedral, inclusions-rich pyrite, 500µm


52280Golden Mile Fimiston Stage II

Pyrite-tourmaline vein in Golden Mile Dolerite (U8)

Fine-grained euhedral pyrite, 200µm


52299

Golden Mile Fimiston Stage IIPyrite-magnetite-chlorite-tourmaline veins in chlorite-carbonate altered Paringa Basalt



323





Reference

52299

Golden Mile Fimiston Stage IIPyrite-magnetite-chlorite-tourmaline veins in chlorite-carbonate altered Paringa Basalt



52198

Golden Mile Fimiston Stage IIIPyrite-sericite-carbonate vein selvedge in Golden Mile Dolerite (U6)

Medium-grained, anhedral (skeletal) pyrite, 300µm


52198


Medium-grained, euhedral, inclusion-rich grains, 300µm


LGX

Golden Mile Fimiston Stage III

Pyrite-tellurides in quartz-carbonate veinlet in Golden Mile Dolerite (U9)

Coarse-grained, anhedral, 800µm


LGX

Golden Mile Fimiston Stage III

Pyrite-tellurides in quartz-carbonate veinlet in Golden Mile Dolerite (U9)

Fine-grained, anhedral, 200µm


UG10


Coarse-grained, euhedral, 800µm


UG10


Coarse-grained, framboidal, skeletal, 500µm


UG3Golden Mile Fimiston Stage IV

Pyrite-sericite selvedge to banded carbonate±quartz vein





Fine-grained, subhedral, 200µm




Fine-grained, subhedral, 200µm


CD2949 169.45

St Ives 1OR Pre-goldAmphibole-pyrrhotite vein in epidote-magnetite altered mafic rock

Very coarse-grained anhedral pyrrhotite, 1500µm


CD2949 169.45

St Ives 1OR Pre-gold Amphibole-pyrrhotite vein in epidote-magnetite altered mafic rock

Medium-grained subhedral pyrite within above pyrrhotite grain, 400µm


CD2949 169.45




CD2949 169.45




LD7113A 135.5St Ives 2OR Main gold stage Feldspar-carbonate-

pyrite altered porphyry

Medium-grained, zoned, inclusion rich pyrite, 500µm




Coarse-grained, zoned, inclusion rich pyrite, 900µm




Fine-grained, subhedral pyrite, 200µm














324

APPENDICES

325

APPENDIX 8 LA-ICP-MS Mineral Chemistry

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95

New Celebration Stage I Mylonite 133565_1-1 Conc. (ppm) 438.71 6.26 9.82 465000.00 3295.45 329.63 50.10 5.56 200.39 18.56 25.71 1.60DL 0.40 0.70 0.50 6.19 0.05 0.19 0.73 0.31 0.52 3.97 0.01 0.54Precision(%) 9.54 12.01 10.99 3.35 5.33 4.49 18.18 11.27 4.63 10.89 5.98 17.73

New Celebration Stage I Mylonite 133565_5-1 Conc. (ppm) 729.22 56.05 117.28 465000.00 92.73 147.00 8.85 26.13 5.37 8.51 5.83 BDDL 0.37 0.51 0.42 22.40 0.05 0.14 0.46 0.20 0.40 3.70 0.01 0.45Precision(%) 16.03 25.14 29.76 5.08 10.21 10.38 17.36 24.45 8.31 19.22 25.25


New Celebration Stage I Mylonite 133565_6-1 Conc. (ppm) 2167.63 20.27 144.03 465000.00 257.15 432.17 13.41 10.21 11.20 14.42 25.80 40.87DL 0.23 0.50 0.38 11.99 0.05 0.19 0.41 0.25 0.50 2.89 0.03 0.50Precision(%) 15.53 9.72 16.92 5.66 9.81 5.04 13.36 13.22 8.43 11.24 11.14 44.93







New Celebration Stage I Porphyry 1213279_1-1 Conc. (ppm) 179.92 32.74 1334.00 465000.00 621.90 683.71 2.45 20.71 6.92 13.35 14.66 2.74DL 0.42 0.89 0.60 9.18 0.08 0.19 0.68 0.58 0.69 5.75 0.02 0.58Precision(%) 14.41 14.27 12.03 6.41 5.94 7.30 14.44 8.56 8.85 18.77 33.04 25.94

New Celebration Stage I Porphyry 1213279_3-1 Conc. (ppm) 106.89 333.24 9.05 465000.00 281.81 1378.60 4.40 105.51 8.60 10.57 1.68 BDDL 0.44 0.60 0.52 7.58 0.05 0.30 0.61 0.23 0.57 4.19 0.01 0.47Precision(%) 28.59 9.63 31.94 3.51 8.27 6.62 10.44 9.09 8.99 17.07 26.25

New Celebration Stage I Porphyry 1213279_4-1 Conc. (ppm) 7.71 BD BD 465000.00 749.63 1571.14 BD BD 2.59 20.15 BD BDDL 0.47 0.62 0.56 6.56 0.06 0.18 0.73 0.35 0.63 3.95 0.01 0.47Precision(%) 6.69 3.23 4.91 3.26 52.43 11.83 9.12

New Celebration Stage I Porphyry 1213279_5-4 Conc. (ppm) 138.22 5.78 0.28 465000.00 481.97 2169.29 BD 0.67 8.84 15.50 9.68 1.13DL 0.65 0.95 0.79 11.45 0.09 0.25 1.17 0.52 0.66 6.30 0.02 0.73Precision(%) 27.25 23.14 109.51 13.78 14.02 14.37 38.27 13.25 20.63 27.72 33.17




326

Sample No

133565_1-1 Conc. (ppm)DLPrecision(%)

















Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U238

39.71 BD 0.76 4.69 77.13 25.54 3.88 4.89 1.39 0.03 21.57 14.87 2.21 0.550.14 2.26 0.15 0.09 1.28 0.06 0.01 0.05 0.05 0.02 0.03 0.01 0.01 0.01

16.20 9.38 4.19 9.49 9.48 19.04 11.15 6.90 34.71 3.85 3.28 12.03 9.001.86 BD 0.65 1.68 10.13 29.23 0.28 6.65 0.26 0.05 6.26 3.34 0.07 0.050.08 2.54 0.10 0.06 1.22 0.05 0.01 0.05 0.03 0.01 0.03 0.01 0.01 0.01

25.07 9.87 8.79 10.51 25.51 30.02 14.36 14.46 25.80 12.90 9.40 21.07 26.96BD 1.67 0.56 0.58 BD 7.27 0.22 0.33 0.04 0.02 3.69 0.67 0.02 0.02

0.06 1.50 0.10 0.06 1.30 0.09 0.01 0.03 0.02 0.01 0.02 0.01 0.01 0.0139.34 9.60 22.47 25.75 24.50 40.86 28.56 36.27 21.75 20.25 30.52 28.21

0.94 BD 0.65 4.07 9.63 1.72 0.69 56.30 0.33 BD 9.81 5.08 0.38 0.260.08 2.19 0.10 0.07 1.58 0.10 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.019.70 9.49 7.72 11.50 14.85 14.84 18.04 12.26 6.81 7.57 12.39 13.101.95 BD 2.05 10.92 28.73 3.93 1.09 316.90 0.63 0.02 10.86 8.16 0.34 0.170.08 2.25 0.12 0.07 1.39 0.07 0.01 0.03 0.03 0.01 0.02 0.01 0.01 0.018.06 13.20 10.99 7.79 16.52 12.67 15.35 18.74 25.17 7.06 5.90 12.55 9.790.41 BD 0.55 1.36 4.37 0.17 2.13 11.36 0.14 BD 4.50 1.43 2.17 1.300.07 2.09 0.12 0.07 1.21 0.04 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.01

13.13 10.36 7.81 14.31 17.99 47.69 8.48 16.79 6.02 6.17 31.94 32.171.04 BD 0.93 1.08 6.65 79.70 1.87 12.42 0.84 0.04 21.86 4.33 0.85 0.280.08 2.56 0.12 0.11 1.48 0.11 0.01 0.04 0.04 0.01 0.03 0.01 0.01 0.01

19.76 8.75 8.66 12.08 12.74 15.59 11.99 16.49 20.95 4.37 6.00 10.63 11.63BD BD 0.51 0.17 2.01 19.56 BD 0.45 BD 0.02 3.33 1.31 0.03 0.04

0.09 2.35 0.10 0.06 1.20 0.06 0.01 0.04 0.03 0.01 0.03 0.02 0.01 0.0110.45 16.93 28.78 12.56 12.42 24.42 9.49 8.47 27.85 46.14

0.27 BD 0.64 0.60 4.48 16.48 0.02 2.15 0.07 BD 13.09 5.91 0.07 0.060.07 2.82 0.11 0.08 1.26 0.09 0.01 0.04 0.04 0.01 0.03 0.01 0.01 0.00

21.93 9.30 9.71 15.85 9.10 31.03 13.02 40.11 11.83 9.83 18.91 14.700.89 BD 0.69 0.33 7.32 79.65 BD 0.92 1.93 0.05 11.73 3.21 0.14 0.170.08 2.05 0.10 0.06 1.63 0.06 0.01 0.04 0.02 0.02 0.02 0.01 0.01 0.01

28.82 9.17 13.36 15.60 12.53 11.47 63.34 17.45 13.95 8.04 13.75 20.190.27 BD 1.18 1.50 5.96 74.99 7.61 BD 0.17 BD 43.82 8.53 0.07 0.200.10 2.99 0.15 0.09 1.85 0.09 0.01 0.06 0.06 0.02 0.04 0.02 0.01 0.01

26.80 8.51 11.33 18.18 14.90 22.94 23.22 9.68 8.43 24.18 36.232.39 BD 0.61 0.97 11.23 6.03 8.42 1.77 2.86 BD 39.20 11.23 0.14 0.060.09 1.97 0.13 0.06 1.13 0.07 0.01 0.04 0.06 0.02 0.04 0.01 0.01 0.01

26.18 11.51 9.27 12.93 50.82 42.37 30.32 40.01 16.84 6.47 29.07 25.150.12 BD 0.42 BD 1.16 BD BD BD 0.12 BD 0.11 0.19 BD BD0.08 2.80 0.12 0.08 1.08 0.06 0.01 0.04 0.04 0.01 0.03 0.02 0.01 0.01

34.70 15.13 40.09 25.56 17.42 10.200.38 BD 1.30 0.31 3.13 7.09 0.03 4.90 0.42 0.02 8.31 2.25 0.15 0.140.19 3.86 0.24 0.16 2.24 0.13 0.01 0.09 0.12 0.02 0.05 0.02 0.01 0.01

41.08 13.51 28.97 33.77 21.38 32.58 29.09 35.78 44.73 19.48 17.58 54.37 23.050.35 BD 0.90 1.42 18.31 60.90 0.14 7.76 0.46 0.03 42.98 15.95 0.27 0.450.13 2.78 0.16 0.07 1.46 0.06 0.01 0.03 0.07 0.02 0.02 0.01 0.01 0.01

25.47 8.48 10.19 7.84 15.84 13.40 25.35 24.70 32.04 13.81 7.53 17.20 19.471.21 BD 1.17 1.54 32.86 0.65 69.45 13.84 1.17 BD 154.47 31.38 4.39 0.540.13 2.48 0.13 0.07 1.00 0.09 0.01 0.04 0.06 0.02 0.04 0.01 0.01 0.01

12.65 7.92 9.18 7.87 21.70 21.47 15.62 15.26 24.70 7.03 25.54 15.981.34 BD 1.47 0.51 7.94 462.89 0.17 1.63 2.10 0.17 15.19 2.19 0.55 1.480.11 3.22 0.16 0.09 1.38 0.09 0.01 0.06 0.05 0.02 0.04 0.01 0.01 0.01

15.61 10.15 15.66 15.16 13.83 26.30 20.68 14.58 16.76 12.57 10.31 26.49 24.98

327

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95New Celebration Stage I Porphyry 133542_1-2 Conc. (ppm) 1180.30 167.74 3.22 465000.00 312.99 425.54 29.12 3.16 12.12 9.59 15.75 BD

DL 0.43 0.57 0.42 13.21 0.06 0.13 0.67 0.35 0.43 4.05 0.02 0.36Precision(%) 28.65 23.90 19.36 3.74 9.85 5.74 34.50 14.06 11.80 17.61 25.65

New Celebration Stage I Porphyry 133542_2-1 Conc. (ppm) 111.83 BD 0.46 465000.00 478.70 1506.46 1.00 0.88 3.33 11.19 12.75 BDDL 0.38 0.70 0.43 8.25 0.05 0.18 0.75 0.39 0.53 4.02 0.03 0.50Precision(%) 40.91 39.00 3.65 3.78 3.70 88.79 23.97 9.24 15.94 28.10

New Celebration Stage I Porphyry 133542_3-1 Conc. (ppm) 35.16 6.45 BD 465000.00 333.36 2336.49 4.44 4.50 3.34 7.27 6.91 BDDL 0.39 0.86 0.58 5.88 0.05 0.22 0.71 0.42 0.54 4.49 0.01 0.43Precision(%) 32.87 27.07 3.96 6.88 3.52 11.05 22.91 8.90 25.10 37.18

New Celebration Stage I Porphyry 133542_4-1 Conc. (ppm) 1225.89 30.56 BD 465000.00 161.69 1573.42 29.44 1.41 9.94 12.78 26.57 BDDL 0.67 0.78 0.57 7.70 0.05 0.19 0.85 0.42 0.62 5.09 0.00 0.47Precision(%) 6.33 9.52 3.53 5.99 4.51 21.56 16.99 5.64 16.73 12.01


New Celebration Stage I Porphyry 133543_1C Conc. (ppm) 8.61 3.38 409.53 465000.00 242.20 3471.50 2.10 13.64 17.77 12.77 0.02 BDDL 0.55 0.55 0.41 5.71 0.04 0.13 0.44 0.22 1.97 6.64 0.01 0.60Precision(%) 8.57 14.45 11.54 6.39 6.84 6.99 11.90 9.96 7.34 23.11 33.64

New Celebration Stage I Porphyry 133543_1R Conc. (ppm) 9.38 1.36 BD 465000.00 167.41 2908.68 1.63 1.11 17.33 BD 0.10 BDDL 0.31 0.71 0.46 4.69 0.03 0.12 0.37 0.25 1.56 10.66 0.02 0.45Precision(%) 7.72 43.20 3.77 8.98 5.50 12.16 14.70 5.88 26.62

New Celebration Stage I Porphyry 133543_2C Conc. (ppm) 8.29 BD 0.58 465000.00 1098.88 622.85 210.72 1.36 11.78 14.07 70.75 BDDL 0.39 0.74 0.31 4.77 0.03 0.09 0.52 0.25 1.71 4.33 0.01 0.52Precision(%) 5.49 21.75 2.59 6.41 3.48 38.32 12.80 6.87 13.32 23.18

New Celebration Stage I Porphyry 133543_2R Conc. (ppm) 7.51 BD BD 465000.00 5.07 289.28 5.93 1.40 16.45 34.66 BD BDDL 0.53 0.80 0.40 5.30 0.04 0.15 0.44 0.22 1.97 4.08 0.01 0.51Precision(%) 6.73 3.84 4.15 3.79 31.63 12.77 7.78 6.58

New Celebration Stage I Porphyry 133543_4 Conc. (ppm) 2463.90 35.10 59.60 465000.00 2094.64 2583.70 184.43 18.26 13.96 27.83 62.06 BDDL 0.40 0.52 0.33 6.79 0.04 0.17 0.52 0.27 2.36 4.51 0.01 0.68Precision(%) 16.57 13.66 10.81 3.89 7.69 7.02 21.77 29.06 9.03 8.28 18.69

New Celebration Stage II Contact 1213371_1-1 Conc. (ppm) 230.34 7.62 BD 465000.00 3261.77 12464.69 1.29 1.34 24.43 8.61 2.37 BDDL 0.25 0.70 0.38 6.15 0.07 0.17 0.57 0.42 0.50 4.65 0.01 0.43Precision(%) 11.12 12.79 310.17 3.96 8.50 3.92 19.72 18.42 4.30 22.60 33.23 81.12

New Celebration Stage II Contact 1213371_1-2 Conc. (ppm) 2475.54 90.57 0.10 465000.00 440.39 11649.64 0.86 1.72 28.40 5.38 13.43 13.22DL 0.45 0.88 0.47 6.93 0.08 0.19 0.58 0.32 0.49 5.19 0.01 0.35Precision(%) 13.47 9.83 184.59 3.64 3.81 3.53 32.05 13.42 4.33 39.84 14.07 22.00

New Celebration Stage II Contact 1213371_1-3 Conc. (ppm) 451.39 22.62 BD 465000.00 3028.28 15803.98 30.98 1.40 42.92 12.70 0.10 BDDL 0.35 0.61 0.49 6.89 0.06 0.38 0.45 0.36 0.53 4.43 0.01 0.39Precision(%) 15.85 13.62 3.67 8.51 3.26 17.69 14.86 4.72 15.79 30.06

New Celebration Stage II Contact 1213371_1-4 Conc. (ppm) 10.24 13.71 BD 465000.00 350.10 7656.89 BD 1.00 6.64 BD BD BDDL 0.47 0.59 0.49 7.56 0.06 0.19 0.60 0.43 0.51 5.61 0.02 0.40Precision(%) 6.54 17.56 351.17 3.72 13.11 4.59 102.67 19.83 6.63 50.11


New Celebration Stage II Contact 1213371_2-2 Conc. (ppm) 11.90 28.43 BD 465000.00 1239.04 11979.29 BD 1.48 31.97 9.40 BD BDDL 0.44 0.67 0.43 12.54 0.10 0.59 0.63 0.32 0.47 4.85 0.01 0.43Precision(%) 9.00 14.23 119.77 3.67 4.21 4.18 14.37 3.94 22.10


New Celebration Stage II Contact 1213371_3-2 Conc. (ppm) 56.02 13.86 BD 465000.00 1335.30 11648.46 31.73 6.89 85.24 6.14 6.68 BD

328

Sample No133542_1-2 Conc. (ppm)

DLPrecision(%)





133543_1C Conc. (ppm)DLPrecision(%)

133543_1R Conc. (ppm)DLPrecision(%)

133543_2C Conc. (ppm)DLPrecision(%)

133543_2R Conc. (ppm)DLPrecision(%)

133543_4 Conc. (ppm)DLPrecision(%)








1213371_3-2 Conc. (ppm)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23811.16 BD 1.59 1.84 43.19 1.38 1.34 73.84 10.70 BD 10.42 3.67 0.17 0.110.11 2.60 0.11 0.08 1.04 0.08 0.01 0.03 0.04 0.01 0.03 0.01 0.00 0.01

43.76 16.87 19.89 15.48 20.77 24.18 32.13 22.87 11.09 13.00 34.95 19.52BD BD 0.66 0.09 BD BD 0.04 1.29 0.09 BD 0.40 0.07 0.15 0.19

0.12 3.19 0.12 0.09 1.02 0.08 0.01 0.05 0.03 0.02 0.03 0.02 0.01 0.009.01 45.47 46.52 22.08 44.05 18.84 23.50 28.23 26.79

1.19 BD 0.72 BD 5.91 BD 0.06 1.21 1.55 BD 1.62 1.16 0.12 0.030.08 2.34 0.14 0.09 1.21 0.07 0.01 0.03 0.05 0.02 0.03 0.02 0.01 0.01

10.23 9.56 13.83 47.69 36.74 16.88 8.47 7.05 32.17 40.78BD BD 0.81 1.80 8.06 0.12 1.08 26.17 2.08 BD 7.65 2.59 0.57 0.13

0.13 2.38 0.15 0.07 1.37 0.09 0.01 0.06 0.04 0.02 0.03 0.01 0.01 0.019.30 7.80 12.75 35.79 13.26 7.50 15.03 4.35 6.32 11.42 14.80

1.10 BD 0.60 0.21 14.71 0.08 BD BD 0.61 BD 5.96 2.47 0.01 BD0.14 2.18 0.14 0.09 1.41 0.04 0.01 0.05 0.04 0.02 0.03 0.02 0.00 0.01

12.36 11.66 24.08 10.25 41.99 12.56 14.88 6.01 39.100.53 BD 0.72 1.03 14.07 0.59 0.09 BD 0.21 BD 7.76 15.33 BD 0.000.10 2.71 0.12 0.08 1.83 0.08 0.01 0.03 0.04 0.01 0.02 0.01 0.01 0.00

14.68 9.64 12.98 9.54 18.73 13.49 17.29 5.98 7.60 36.020.50 3.16 0.49 0.10 18.42 BD BD BD 0.35 BD 0.98 3.21 0.01 BD0.07 1.94 0.13 0.02 1.00 0.05 0.01 0.03 0.03 0.02 0.02 0.01 0.00 0.00

15.61 25.82 11.18 18.11 7.45 19.39 12.13 10.22 43.950.99 BD 0.41 0.23 36.68 BD BD 0.07 0.50 BD 6.23 23.44 1.26 0.400.08 1.96 0.09 0.04 1.34 0.07 0.01 0.04 0.03 0.01 0.02 0.01 0.00 0.017.88 9.37 13.76 7.19 29.86 8.79 5.04 5.96 20.82 22.420.55 BD 0.47 BD 14.90 0.62 BD BD 0.30 BD 0.57 1.68 BD BD0.06 2.54 0.11 0.08 1.27 0.09 0.01 0.03 0.03 0.02 0.02 0.01 0.01 0.00

15.59 11.54 8.45 107.37 16.48 11.86 9.040.28 BD 0.66 BD 1.74 2.14 1.06 0.61 0.09 BD 12.45 5.98 1.47 0.520.09 2.40 0.12 0.07 1.48 0.08 0.01 0.03 0.05 0.01 0.02 0.01 0.01 0.01

23.31 10.29 35.19 12.55 16.93 15.74 33.49 11.19 5.84 17.64 14.720.13 BD 0.59 0.37 BD BD BD 2.98 0.11 BD 0.77 0.49 0.07 0.060.10 2.43 0.10 0.05 1.28 0.08 0.01 0.02 0.04 0.01 0.03 0.01 0.01 0.01

34.63 9.30 12.55 13.38 34.59 7.37 6.08 28.87 27.305.25 BD 0.69 2.41 20.79 0.23 0.05 27.24 12.37 BD 5.49 1.45 0.45 0.550.10 2.38 0.13 0.06 1.31 0.06 0.00 0.03 0.04 0.02 0.03 0.01 0.01 0.01

28.49 9.78 11.86 18.80 23.28 16.14 10.37 31.30 16.10 10.17 11.63 11.2915.23 BD 0.64 1.80 54.90 BD BD 11.79 33.67 BD 8.17 5.21 0.04 0.030.12 2.46 0.12 0.08 1.48 0.06 0.01 0.04 0.03 0.02 0.03 0.01 0.00 0.01

23.07 10.02 9.25 21.93 27.21 25.16 15.86 11.60 19.90 23.600.30 BD 0.63 0.16 BD 0.12 BD BD 0.36 BD 1.12 0.12 BD BD0.09 2.45 0.13 0.08 1.54 0.08 0.01 0.04 0.04 0.02 0.03 0.01 0.01 0.01

25.65 10.20 28.85 36.18 36.69 15.55 14.809.34 BD 1.03 1.91 50.38 1.01 0.03 11.14 9.33 0.14 13053.16 48.18 0.14 0.170.12 3.48 0.16 0.08 1.60 0.08 0.01 0.05 0.07 0.02 0.05 0.02 0.01 0.01

14.04 8.57 7.96 9.36 12.69 29.90 19.32 27.49 18.77 20.74 12.99 16.33 16.14BD BD 0.56 BD 2.55 0.31 BD 0.05 0.32 BD BD 0.16 BD BD

0.13 2.12 0.12 0.09 1.68 0.06 0.01 0.04 0.04 0.02 0.74 0.01 0.01 0.0111.40 31.36 19.59 50.90 36.14 13.45

15.83 BD 0.61 2.18 68.59 0.40 BD 0.39 30.77 BD 258.16 10.81 0.13 0.150.09 2.49 0.12 0.06 1.26 0.09 0.01 0.03 0.05 0.01 0.03 0.02 0.01 0.01

15.76 10.06 12.40 14.64 22.36 11.75 23.45 30.22 17.75 46.89 42.004.56 BD 0.49 2.54 12.04 0.19 0.03 0.87 2.66 BD 11.53 5.15 0.10 0.05

329

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95DL 0.57 0.63 0.43 9.36 0.09 0.61 0.69 0.57 0.47 5.89 0.01 0.46Precision(%) 22.05 18.61 3.68 5.12 4.57 23.91 21.77 3.72 36.89 19.31

New Celebration Stage II Contact 1250_12-18_1-2 Conc. (ppm) 13.56 186.11 8.19 465000.00 1464.35 2874.31 13.59 9.78 55.13 11.86 0.05 BDDL 0.21 0.71 0.53 7.91 0.06 0.19 0.51 0.42 0.47 4.81 0.02 0.40Precision(%) 9.38 17.68 18.31 3.45 3.89 6.16 40.74 16.34 4.05 17.87 30.77

New Celebration Stage II Contact 1250_12-18_1-3 Conc. (ppm) 7.66 0.92 1.02 465000.00 12.63 727.62 60.91 1.52 1.12 28.97 BD BDDL 0.55 0.83 0.53 6.20 0.06 0.16 0.65 0.31 0.52 4.42 0.02 0.57Precision(%) 7.56 39.20 27.07 3.42 14.81 14.59 30.52 29.34 20.45 8.17


New Celebration Stage II Contact 1250_12-18_2-2 Conc. (ppm) 8.58 4.47 0.53 465000.00 1857.26 4503.72 BD 1.10 44.13 14.80 0.02 BDDL 0.40 0.56 0.50 9.18 0.10 0.24 0.69 0.37 0.65 3.65 0.01 0.37Precision(%) 7.12 33.69 39.86 3.45 4.82 5.29 19.23 3.95 12.02 44.37

New Celebration Stage II Contact 1250_12-18_3-1 Conc. (ppm) 9.66 15.10 BD 465000.00 881.82 4502.64 BD 1.17 38.21 7.93 BD BDDL 0.53 0.67 0.47 17.90 0.09 0.44 0.80 0.40 0.66 4.69 0.01 0.44Precision(%) 7.37 18.08 3.55 10.61 7.34 23.50 7.38 24.65

New Celebration Stage II Contact 1250_12-18_4-1 Conc. (ppm) 20.72 76.96 29.76 465000.00 3130.63 514.91 11.40 2.91 21.53 6.50 BD BDDL 0.52 0.53 0.54 11.09 0.06 0.27 0.69 0.36 0.52 4.87 0.01 0.40Precision(%) 8.02 11.38 11.76 2.85 4.79 6.69 28.31 17.79 6.01 28.67


New Celebration Stage II Contact 1250_12-18_5-2 Conc. (ppm) 9.60 8.45 1.45 465000.00 1965.18 2271.71 22.68 9.26 55.12 37.90 12.67 455.38DL 0.78 0.95 0.98 16.22 0.10 0.20 1.32 1.06 0.95 9.34 0.02 0.89Precision(%) 19.73 20.50 55.72 18.28 18.41 18.12 34.23 32.08 18.08 18.19 41.02 37.50

New Celebration Stage II Fracture 1213357_1-1 Conc. (ppm) 67.60 BD 0.08 465000.00 45.72 82.05 3.31 0.56 2.62 20.90 2.71 BDDL 0.38 0.64 0.46 8.22 0.05 0.21 0.62 0.34 0.53 6.38 0.02 0.41Precision(%) 29.28 229.02 4.02 10.41 6.92 9.82 28.53 11.68 13.52 26.37

New Celebration Stage II Fracture 1213357_1-2 Conc. (ppm) 9.16 BD BD 465000.00 76.44 399.93 BD 0.79 2.29 14.47 0.05 BDDL 0.39 0.59 0.45 24.28 0.06 0.19 0.53 0.40 0.67 5.06 0.02 0.43Precision(%) 6.12 4.18 4.97 5.03 26.87 14.58 15.42 66.34

New Celebration Stage II Fracture 1213357_1-3 Conc. (ppm) 535.79 2.23 BD 465000.00 16.82 26.04 1.74 1.10 1.82 17.86 63.51 BDDL 0.40 0.74 0.53 23.16 0.09 0.20 0.56 0.31 0.60 6.37 0.01 0.42Precision(%) 23.31 22.29 4.14 6.74 6.14 28.27 16.40 16.12 15.11 34.34

New Celebration Stage II Fracture 1213357_2-1 Conc. (ppm) 63.96 BD BD 465000.00 335.03 156.18 1.26 0.64 3.63 26.59 1.18 BDDL 0.26 0.58 0.41 0.00 0.05 0.16 0.49 0.29 0.48 5.25 0.02 0.37Precision(%) 20.74 5.84 5.90 5.73 21.71 22.81 8.96 9.96 24.92

New Celebration Stage II Fracture 1213357_3-1 Conc. (ppm) 3716.19 5.27 0.25 465000.00 3.27 8.92 5.63 1.67 73.92 18.53 360.41 BDDL 0.30 0.50 0.51 11.06 0.07 0.16 0.53 0.33 0.62 5.44 0.02 0.43Precision(%) 21.25 19.48 77.65 4.05 5.14 5.15 6.99 14.65 4.14 13.18 12.23




New Celebration Stage II Fracture 1213357_4-2 Conc. (ppm) 100.72 1.21 BD 465000.00 16.73 27.29 14.11 38.22 1.80 11.11 2.58 BDDL 0.45 0.36 0.34 0.00 0.06 0.18 0.36 0.25 0.52 5.31 0.00 0.37

330

Sample NoDLPrecision(%)

1250_12-18_1-2 Conc. (ppm)DLPrecision(%)
















1213357_4-2 Conc. (ppm)DL

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2380.10 2.22 0.14 0.09 1.18 0.09 0.01 0.05 0.04 0.02 0.03 0.01 0.01 0.01

14.78 13.18 6.66 13.39 34.79 68.52 24.61 20.29 19.71 5.92 28.45 17.95106.89 BD 0.66 0.20 848.88 0.12 BD BD 144.39 0.03 4076.32 50.75 BD BD

0.17 2.74 0.14 0.08 0.97 0.09 0.01 0.04 0.48 0.01 0.04 0.02 0.01 0.0122.67 10.17 24.46 17.02 39.98 22.54 23.18 17.34 17.80

0.49 BD 0.68 0.07 2.83 0.22 BD BD 2.52 BD 8.18 0.37 BD BD0.13 2.73 0.11 0.05 1.55 0.05 0.01 0.04 0.05 0.02 0.04 0.02 0.01 0.01

38.26 9.70 39.20 27.16 25.21 62.63 12.75 11.474.36 BD 0.67 0.22 118.98 0.11 0.03 BD 12.06 BD 2.85 5.80 BD BD0.14 2.67 0.12 0.07 1.75 0.06 0.01 0.02 0.05 0.02 0.04 0.01 0.01 0.01

26.73 10.04 18.84 36.93 35.72 21.95 30.28 12.10 14.890.23 BD 0.51 BD 1.82 BD 0.01 BD 1.58 BD 0.31 0.16 BD BD0.11 2.46 0.13 0.07 1.46 0.10 0.00 0.04 0.04 0.02 0.03 0.02 0.01 0.01

26.03 11.62 33.70 42.56 59.21 11.51 11.640.20 BD 0.61 BD 2.66 BD BD BD 0.48 BD 0.67 0.26 BD BD0.10 2.75 0.15 0.06 1.17 0.09 0.01 0.05 0.05 0.02 0.03 0.01 0.01 0.01

40.68 10.58 28.40 47.21 26.63 15.39BD BD 0.51 0.17 3.07 0.18 0.03 0.03 0.23 BD 4.84 0.95 BD 0.01

0.11 2.72 0.14 0.11 1.02 0.05 0.01 0.03 0.06 0.02 0.03 0.01 0.01 0.0012.15 31.03 18.23 22.24 21.77 47.72 45.75 8.60 6.39 33.05

9.08 BD 0.63 0.34 13.88 2.60 0.08 0.09 0.92 0.12 15.35 1.99 BD 0.040.23 4.92 0.27 0.13 2.42 0.11 0.02 0.07 0.07 0.03 0.06 0.03 0.01 0.01

27.38 21.78 23.43 18.25 36.28 29.46 43.62 35.69 21.96 15.38 14.52 26.680.29 BD 0.83 0.19 5.09 0.92 BD BD 0.19 0.04 4.97 1.19 0.08 0.200.24 4.52 0.25 0.16 3.06 0.15 0.02 0.09 0.10 0.03 0.06 0.03 0.02 0.01

47.57 21.99 41.79 29.79 44.75 36.66 42.71 23.38 19.60 53.36 40.812.62 0.61 0.59 0.21 5.69 BD 0.02 1.65 2.27 0.03 4.98 2.83 0.02 0.020.10 2.03 0.13 0.11 1.37 0.08 0.01 0.03 0.04 0.01 0.04 0.01 0.01 0.01

10.39 136.57 11.75 28.82 15.78 40.47 24.15 10.87 29.20 11.57 10.87 32.11 27.58BD BD 0.55 BD BD BD BD BD BD BD BD 0.19 BD BD

0.09 1.73 0.15 0.09 1.06 0.06 0.01 0.06 0.05 0.02 0.04 0.02 0.01 0.0112.50 9.47

0.14 BD 0.88 0.55 2.48 95.52 1.98 8.80 0.11 BD 3.20 0.40 1.14 0.710.14 2.16 0.15 0.10 1.11 0.10 0.01 0.03 0.05 0.03 0.02 0.01 0.01 0.01

41.16 9.78 12.49 24.22 49.30 65.25 9.16 28.69 5.93 9.38 20.97 21.58BD BD 0.57 0.12 5.42 1.48 0.04 0.88 0.27 0.02 17.55 4.39 0.07 0.04

0.11 2.39 0.12 0.08 0.99 0.08 0.01 0.05 0.03 0.01 0.05 0.02 0.01 0.0112.75 34.83 14.07 33.30 20.72 20.64 25.51 39.19 16.37 10.34 23.34 22.87

3.80 BD 2.46 8.29 21.67 0.84 1.49 90.84 2.48 0.18 58.67 20.69 36.68 11.520.10 2.12 0.13 0.09 1.23 0.07 0.01 0.05 0.03 0.01 0.03 0.02 0.01 0.019.71 16.42 6.00 10.45 23.23 19.06 20.42 15.42 7.23 4.33 9.86 14.06 12.140.66 BD 0.45 0.14 1.91 BD BD 0.51 0.83 BD 2.76 0.77 0.08 0.030.09 2.12 0.14 0.08 1.70 0.07 0.01 0.06 0.05 0.02 0.04 0.01 0.01 0.00

16.02 14.56 29.90 40.00 22.47 26.36 18.83 10.88 36.46 29.515.45 BD 1.36 1.61 1282.98 38.36 1.46 33.00 1.60 0.04 246.39 1670.74 5.07 2.340.11 2.22 0.13 0.08 1.10 0.06 0.01 0.04 0.03 0.02 0.03 0.01 0.00 0.01

31.97 12.06 16.04 29.91 60.29 21.92 13.29 13.93 32.16 25.74 30.03 20.14 14.901.56 BD 1.19 0.82 31.50 54.87 2.69 35.20 1.60 BD 211.12 17.33 0.86 0.220.09 1.97 0.12 0.06 0.99 0.07 0.01 0.05 0.04 0.02 0.03 0.01 0.01 0.01

15.11 13.35 17.21 19.56 26.46 33.47 17.64 19.43 25.23 21.41 23.24 18.911.26 BD 0.48 0.51 7.28 2.38 0.11 2.73 0.66 BD 7.32 3.31 0.08 0.050.08 1.86 0.11 0.08 1.00 0.09 0.01 0.04 0.04 0.02 0.03 0.02 0.01 0.01

331

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Precision(%) 15.53 21.86 9.57 16.41 14.29 53.57 52.24 21.82 20.17 41.79

New Celebration Stage II Fracture 1213357_4-3 Conc. (ppm) 43.63 BD BD 465000.00 22.23 62.13 10.38 0.70 16.08 22.20 2.47 0.28DL 0.44 0.65 0.41 0.00 0.07 0.18 0.52 0.41 0.61 6.17 0.01 0.34Precision(%) 12.60 6.50 6.96 10.14 8.76 26.22 6.11 12.68 36.32 49.02





New Celebration Stage II Fracture 1213359_2-3 Conc. (ppm) 261.68 1.90 0.38 465000.00 204.60 308.00 BD 0.91 1.25 20.39 2.35 BDDL 0.44 0.63 0.53 6.87 0.07 0.20 0.81 0.42 0.51 5.03 0.01 0.52Precision(%) 12.82 21.21 53.99 3.87 6.78 5.34 22.71 19.61 11.07 36.21

New Celebration Stage II Fracture 1213359_2-4 Conc. (ppm) 887.78 3.24 BD 465000.00 16.67 25.59 1.82 0.92 9.85 18.40 81.43 1.39DL 0.44 0.80 0.45 7.31 0.06 0.20 0.60 0.62 0.73 6.02 0.02 0.50Precision(%) 13.24 16.88 3.77 7.60 4.59 16.54 29.52 7.14 13.96 18.91 65.39



New Celebration Stage II Fracture 1213359_3-4 Conc. (ppm) 117.00 BD BD 465000.00 3.79 33.74 7.44 1.01 16.78 15.95 66.12 BDDL 0.56 0.76 0.44 7.14 0.06 0.24 0.67 0.32 0.55 5.55 0.02 0.49Precision(%) 10.19 131.69 4.20 6.53 4.21 7.14 19.34 5.65 15.84 16.03


New Celebration Stage II Fracture 1213359_4-3 Conc. (ppm) 2227.69 9.13 0.59 465000.00 55.12 720.42 6.73 0.96 4.13 11.28 153.67 1.90DL 0.65 0.61 0.50 8.50 0.07 0.20 0.50 0.39 0.54 4.78 0.01 0.44Precision(%) 8.99 9.86 33.16 3.72 10.87 16.09 7.03 20.11 8.16 18.16 14.70 36.00

New Celebration Stage II Fracture 1213359_4-4 Conc. (ppm) 364.19 5.05 2.74 465000.00 195.97 1058.71 117.57 24.39 45.85 26.84 419.83 2.44DL 0.43 0.67 0.49 10.76 0.05 0.18 0.65 0.43 0.51 4.86 0.02 0.49Precision(%) 15.65 17.11 13.36 6.85 7.58 7.40 72.98 12.25 13.11 11.57 16.43 18.99

New Celebration JD0475-5_4-3 Conc. (ppm) 16159.13 4.51 384.79 465000.00 10788.34 1007.88 34.08 72.22 847.91 47.20 84.47 BDDL 65.37 0.71 0.47 6.77 0.06 0.19 0.64 0.27 0.66 4.86 0.02 0.56Precision(%) 9.93 15.69 13.53 11.78 13.04 9.62 30.37 13.84 12.05 12.77 19.15

New Celebration JD0475-5_4-4 Conc. (ppm) 10504.48 3.90 504.19 465000.00 7680.38 728.55 1.71 59.85 909.65 49.21 4.73 BDDL 0.46 0.64 0.39 6.26 0.05 0.17 0.46 0.24 0.51 4.09 0.02 0.52Precision(%) 14.19 15.94 14.86 6.54 7.29 5.29 16.18 14.55 6.57 7.86 23.31

Golden Mile Chron. Samples Synvolcanic sulfide 3765_1-1 Conc. (ppm) 1541.71 26.55 1631.59 465000.00 84.89 3470.48 41535.53 253.86 37.80 50.63 76.90 BDDL 0.33 0.87 0.57 15.68 0.05 0.33 1.75 0.30 0.53 4.42 0.03 0.55Precision(%) 10.08 9.61 8.00 4.96 9.21 9.72 14.92 9.99 6.60 7.64 4.43

Golden Mile Chron. Samples Synvolcanic sulfide 3765_2-1 Conc. (ppm) 1528.28 11.91 106.09 465000.00 222.34 1903.11 BD 2.97 1.78 27.03 43.01 BDDL 0.61 0.73 0.60 22.59 0.06 0.27 0.64 0.53 0.49 4.83 0.01 0.71Precision(%) 11.70 7.27 13.62 2.55 2.71 2.83 15.48 24.64 9.17 4.62

332

Sample NoPrecision(%)














JD0475-5_4-3 Conc. (ppm)DLPrecision(%)

JD0475-5_4-4 Conc. (ppm)DLPrecision(%)



Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23811.40 12.98 13.88 17.02 33.22 21.13 14.85 14.09 10.76 20.88 18.37 29.86

1.75 BD 0.54 0.46 28.46 12.39 0.37 1.36 1.10 BD 14.49 28.18 0.12 0.050.10 2.52 0.13 0.04 1.51 0.07 0.01 0.05 0.04 0.03 0.03 0.02 0.01 0.018.09 11.97 9.77 7.73 31.30 23.58 17.76 8.88 5.81 6.28 18.96 49.281.90 0.34 0.58 1.39 25.00 1.12 1.00 2.62 1.10 BD 87.59 9.90 0.82 1.040.09 2.40 0.17 0.09 1.03 0.10 0.01 0.04 0.05 0.02 0.03 0.01 0.01 0.018.70 276.59 13.35 7.91 9.02 25.86 35.63 17.15 14.07 19.07 7.81 17.68 20.883.29 BD 0.53 1.12 5.29 59.23 2.75 4.10 0.55 0.56 3392.60 66.61 7.19 5.040.13 2.44 0.14 0.07 1.20 0.06 0.01 0.06 0.05 0.02 0.03 0.02 0.01 0.01

10.97 12.39 25.81 14.14 25.68 56.03 24.34 24.14 10.80 12.26 7.39 23.35 24.65245.96 BD 0.54 BD 252.28 0.70 BD BD 558.28 BD 29.20 4.82 36.32 11.80

0.11 2.78 0.15 0.09 1.20 0.09 0.01 0.05 0.02 0.02 0.03 0.01 0.01 0.0137.27 12.98 41.02 23.12 31.81 15.57 13.99 29.06 22.55

0.13 2.50 0.56 BD 2.41 0.15 0.02 BD 0.15 BD 54.47 2.66 0.66 1.320.10 1.83 0.15 0.08 1.40 0.09 0.01 0.05 0.08 0.02 0.04 0.01 0.01 0.01

44.70 32.64 12.55 27.31 30.55 25.79 33.04 16.95 15.17 20.86 29.291.17 BD 0.80 0.21 1.49 BD 2.42 6.05 1.24 BD 3.19 0.55 1.00 0.060.12 1.94 0.15 0.07 1.67 0.09 0.01 0.04 0.09 0.02 0.03 0.01 0.01 0.01

14.80 9.71 23.43 46.39 34.66 13.68 15.80 17.57 7.79 29.83 29.910.92 BD 0.93 1.22 10.86 0.30 3.57 16.72 0.96 BD 14.60 2.30 2.54 1.190.10 2.67 0.12 0.06 1.22 0.09 0.01 0.04 0.07 0.02 0.03 0.02 0.01 0.01

21.88 8.88 11.40 11.26 27.78 33.71 11.66 37.06 10.51 7.24 18.19 18.245.15 BD 0.61 0.39 30.20 17.27 3.98 7.31 0.99 0.25 3448.37 259.62 3.46 2.590.10 1.84 0.13 0.09 1.22 0.05 0.01 0.06 0.05 0.02 0.03 0.02 0.01 0.01

16.78 11.53 16.71 13.91 31.53 40.74 12.03 9.47 22.97 22.14 24.82 12.97 13.8658.65 BD 0.56 0.26 11.98 BD 2.08 1.90 482.72 BD 14.76 1.63 0.76 0.440.12 2.05 0.13 0.08 1.32 0.08 0.01 0.04 0.05 0.02 0.46 0.02 0.01 0.00

30.19 12.28 18.99 13.49 57.54 17.58 18.16 12.17 7.44 24.35 20.920.74 BD 0.62 0.31 23.00 2.83 0.86 2.37 0.65 BD 16.84 10.58 1.35 0.930.13 2.82 0.15 0.08 1.25 0.10 0.01 0.06 0.07 0.02 0.04 0.02 0.01 0.01

11.26 11.28 15.64 7.33 18.47 25.22 14.60 10.89 7.18 5.63 15.83 15.011.44 BD 0.58 0.79 13.63 31.60 1.61 4.90 1.06 0.08 176.75 23.80 0.53 0.100.51 2.68 0.12 0.08 1.48 0.09 0.01 0.06 0.06 0.02 0.04 0.02 0.01 0.01

15.27 10.44 10.84 9.84 20.74 19.37 15.37 11.74 17.25 17.04 9.97 18.06 22.811.07 BD 1.79 1.94 10.27 0.37 14.50 58.00 0.98 BD 23.12 11.29 6.56 3.220.14 2.38 0.12 0.08 1.40 0.08 0.01 0.04 0.05 0.02 0.04 0.02 0.01 0.019.59 7.22 7.97 10.92 19.98 21.26 8.47 12.15 9.85 7.45 16.16 16.20

53.61 BD 1.90 4.08 38.29 1351.46 32.90 13.31 559.63 0.24 760.03 126.51 18.94 14.440.20 2.41 0.15 0.07 1.43 0.08 0.01 0.07 0.04 0.02 0.03 0.02 0.01 0.01

28.10 9.01 14.36 13.34 14.49 31.96 12.05 41.62 12.60 12.22 14.27 19.20 11.190.89 BD 26.45 4.36 4.77 1.24 0.10 2.98 BD BD 4.30 3.76 0.06 0.040.14 4.00 0.15 0.09 1.59 0.10 0.01 0.04 0.05 0.02 0.04 0.01 0.01 0.01

25.86 55.33 10.19 19.21 15.79 15.40 13.16 10.34 12.01 20.58 17.340.28 BD 2.96 1.03 2.68 0.43 BD 0.94 0.03 BD 0.97 1.05 0.01 0.010.08 2.32 0.09 0.07 1.18 0.08 0.01 0.03 0.02 0.01 0.03 0.01 0.00 0.00

20.96 64.10 10.47 22.67 20.07 14.46 38.11 10.33 11.48 30.38 23.9710.69 BD 1.66 47.37 BD 9.11 19.47 3.51 BD 3.50 60.00 0.03 3.00 0.980.09 2.42 0.16 0.07 1.33 0.06 0.01 0.04 0.06 0.02 0.04 0.01 0.01 0.00

23.97 6.49 6.74 8.99 23.53 8.19 22.57 5.31 25.26 15.04 5.070.81 BD 1.06 2.93 BD 21.13 0.12 3.53 BD 0.09 3.24 BD 0.60 0.590.09 2.46 0.14 0.08 1.30 0.10 0.01 0.04 0.05 0.02 0.02 0.01 0.01 0.01

10.66 7.61 5.95 6.81 12.46 9.09 14.00 3.75 5.18 5.25

333

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Golden Mile Chron. Samples Synvolcanic sulfide 3765_3-1 Conc. (ppm) 1221.38 11.22 BD 465000.00 108.43 136.93 3.91 1.41 1368.98 15.07 37.00 BD

DL 0.86 1.54 0.99 15.49 0.07 0.30 1.30 0.63 1.35 8.77 0.06 0.98Precision(%) 19.23 21.97 4.47 7.31 5.89 15.66 38.34 3.91 23.57 6.39

Golden Mile Chron. Samples Synvolcanic sulfide 3765_3-2 Conc. (ppm) 1037.75 6.84 BD 465000.00 140.74 153.18 0.74 0.72 1220.69 19.83 34.69 0.58DL 0.27 0.54 0.46 6.41 0.05 0.17 0.52 0.21 0.48 4.50 0.02 0.49Precision(%) 17.91 17.35 62.17 3.73 5.97 3.57 30.20 18.74 5.47 10.67 6.44 39.85

Golden Mile Chron. Samples Synvolcanic sulfide 3765_4-1 Conc. (ppm) 343.16 1.48 1.84 465000.00 60.60 173.48 60.44 171.01 954785.06 299.67 11.51 3.98DL 0.53 0.85 0.62 17.72 0.06 0.15 0.90 0.40 0.00 5.16 0.03 0.73Precision(%) 10.78 25.78 13.52 2.56 4.99 2.83 11.58 16.41 4.98 3.86 4.73 9.75

Golden Mile Chron. Samples Synvolcanic sulfide 3765_4-2 Conc. (ppm) 293.16 BD 30.65 465000.00 37.14 103.66 22.08 6.78 740242.95 177.67 9.07 BDDL 0.35 0.62 0.46 10.90 0.03 0.17 0.59 0.33 0.00 2.88 0.02 0.37Precision(%) 10.50 17.08 4.21 5.58 3.68 16.31 12.76 5.54 4.05 8.72



Golden Mile Chron. Samples Synvolcanic sulfide LG106_1-3 Conc. (ppm) 7.71 14.27 6.14 465000.00 83.39 384.72 332.29 4.39 2555.06 9.50 5.53 BDDL 0.33 0.65 0.51 7.02 0.05 0.20 0.55 0.33 0.46 4.52 0.02 0.48Precision(%) 6.34 9.11 12.84 3.51 4.07 3.27 7.21 20.79 6.50 20.61 21.10







Golden Mile Chron. Samples Pre-gold sulfide JOGD11-2_1-1 Conc. (ppm) 7.11 BD 1.93 465000.00 4160.83 1.29 BD 0.88 115.35 35.22 BD BDDL 0.37 0.66 0.54 7.91 0.06 0.15 0.67 0.49 0.55 3.34 0.02 0.56Precision(%) 6.92 19.27 3.65 3.67 10.51 26.21 3.50 5.78

Golden Mile Chron. Samples Pre-gold sulfide JOGD11-2_2-1 Conc. (ppm) 65.60 BD 78.13 465000.00 2433.41 6.34 108.63 3.99 117.62 51.98 BD BDDL 0.51 0.81 0.72 36.08 0.21 0.28 0.75 0.49 0.58 4.74 0.01 0.63Precision(%) 18.75 11.55 5.77 14.79 10.71 26.07 14.04 10.53 6.71

Golden Mile Chron. Samples Pre-gold sulfide JOGD11-2_3-1 Conc. (ppm) 18.41 BD 1.65 465000.00 5085.64 0.83 2.42 1.85 152.83 27.94 0.37 BDDL 0.48 0.76 0.50 16.18 0.19 0.15 0.93 0.50 0.73 3.69 0.01 0.54Precision(%) 5.80 13.57 3.76 7.38 13.38 17.10 14.70 3.83 7.27 17.35

Golden Mile Chron. Samples Pre-gold sulfide JOGD11-2_4-1 Conc. (ppm) 6.08 BD BD 465000.00 2736.84 2.66 BD 0.99 140.81 38.28 BD BDDL 0.43 0.74 0.59 11.12 0.10 0.19 0.75 0.37 0.49 3.00 0.02 0.48Precision(%) 6.85 3.78 3.31 10.14 20.70 3.76 5.38

Golden Mile Chron. Samples Pre-gold sulfide JOGD11-2_4-2 Conc. (ppm) 6.47 BD BD 465000.00 2286.97 22.00 1.71 0.67 59.29 70.69 BD BD

334

Sample No3765_3-1 Conc. (ppm)

DLPrecision(%)






LG106_1-3 Conc. (ppm)DLPrecision(%)







JOGD11-2_1-1 Conc. (ppm)DLPrecision(%)




JOGD11-2_4-2 Conc. (ppm)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2380.55 BD 1.02 12.38 BD BD 0.04 2.68 BD BD 5.45 0.17 0.53 0.540.11 4.80 0.25 0.14 2.20 0.11 0.01 0.09 0.05 0.02 0.05 0.03 0.01 0.01

15.04 12.01 7.34 46.20 17.80 8.94 13.35 7.63 6.95BD BD 0.64 2.63 BD BD 1.08 1.89 BD BD 0.97 0.12 0.98 0.52

0.05 1.65 0.12 0.06 0.74 0.09 0.01 0.04 0.02 0.02 0.03 0.02 0.00 0.019.34 6.79 45.90 15.47 7.54 93.33 23.78 7.05

0.72 BD 1.08 615.97 9.86 0.40 1.14 0.49 0.30 0.82 33.25 2.45 0.52 0.250.14 2.87 0.18 0.12 1.59 0.07 0.00 0.04 0.04 0.02 0.03 0.01 0.01 0.01

12.34 8.17 3.08 10.02 15.44 16.54 14.61 12.83 9.04 3.72 3.80 19.56 6.240.80 BD 1.01 237.04 4.29 0.35 2.39 0.79 0.15 1.35 27.94 0.98 0.93 0.200.04 2.32 0.14 0.10 0.89 0.05 0.01 0.04 0.03 0.01 0.02 0.01 0.00 0.019.69 7.92 3.76 12.54 14.16 23.70 50.62 13.59 11.59 7.09 6.69 42.39 11.441.00 BD 0.97 26.56 BD 0.83 0.07 0.25 BD 1.42 29.28 0.46 0.40 0.300.08 2.14 0.14 0.07 1.46 0.04 0.01 0.04 0.04 0.01 0.02 0.00 0.01 0.019.28 8.50 3.89 39.01 20.76 18.25 16.26 5.61 5.72 10.87 8.561.45 BD 0.71 32.18 BD 0.14 0.02 0.10 BD 2.76 27.76 0.59 0.14 0.120.08 2.12 0.13 0.06 0.88 0.12 0.01 0.02 0.03 0.01 0.03 0.01 0.01 0.017.83 9.46 6.20 38.67 20.02 19.11 11.20 6.22 6.74 10.41 11.705.82 BD 1.06 70.55 5.28 0.15 0.03 0.07 0.97 0.10 130.99 61.41 0.02 BD0.09 2.28 0.14 0.06 1.36 0.06 0.01 0.03 0.03 0.01 0.02 0.01 0.01 0.016.41 8.22 3.28 14.94 33.87 26.51 31.79 8.50 10.44 3.70 4.47 32.153.25 BD 0.86 27.91 4.88 0.09 BD BD 0.51 0.10 54.44 42.18 0.04 0.100.11 3.26 0.13 0.08 1.81 0.08 0.01 0.04 0.05 0.01 0.04 0.01 0.01 0.015.78 8.90 5.60 17.15 46.68 10.88 12.94 6.39 4.93 14.17 12.080.76 BD 0.80 32.85 2.46 0.18 0.93 0.11 0.10 BD 71.33 14.31 0.02 0.020.11 2.69 0.15 0.08 1.37 0.09 0.01 0.03 0.03 0.02 0.03 0.01 0.00 0.01

14.04 9.24 16.09 26.21 30.92 14.94 47.70 20.38 15.06 13.31 25.01 28.133.78 BD 0.76 23.76 5.70 0.24 0.04 0.05 0.28 0.05 35.80 42.35 0.02 0.060.11 3.01 0.15 0.07 1.45 0.07 0.01 0.04 0.04 0.02 0.02 0.01 0.01 0.017.00 9.62 4.96 14.88 44.85 41.62 39.93 12.78 16.67 8.65 5.75 30.70 26.56

BD BD 0.68 1.46 BD BD 0.06 BD 0.03 BD 0.56 0.56 BD BD0.12 2.74 0.15 0.09 1.42 0.07 0.01 0.03 0.02 0.01 0.03 0.01 0.01 0.01

10.68 39.40 39.51 40.07 36.78 34.031.14 BD 0.76 12.18 2.52 0.18 0.06 0.07 0.15 BD 23.34 31.03 0.02 0.050.10 3.04 0.14 0.07 1.56 0.10 0.01 0.04 0.05 0.02 0.03 0.01 0.00 0.018.92 9.69 3.97 28.86 28.94 14.91 40.39 17.10 5.09 3.85 24.36 22.312.13 BD 0.96 19.44 2.07 BD BD 0.13 0.42 0.18 30.16 26.60 0.02 0.020.10 2.38 0.14 0.09 1.69 0.09 0.01 0.04 0.02 0.01 0.03 0.01 0.01 0.01

11.46 8.21 5.92 33.74 37.71 9.20 9.81 7.90 4.90 27.09 29.85BD BD 0.76 1.12 BD BD BD BD BD BD 0.24 0.25 BD BD

0.10 3.00 0.14 0.06 1.60 0.07 0.01 0.03 0.03 0.01 0.03 0.01 0.00 0.019.33 8.17 11.10 7.51

0.68 BD 2.70 21.01 2.03 131.45 0.04 853.70 0.23 0.14 3.99 3.00 BD BD0.12 3.75 0.14 0.07 1.54 0.07 0.01 0.04 0.04 0.01 0.04 0.02 0.01 0.01

16.11 14.95 7.71 34.50 20.95 23.09 38.23 15.19 17.54 9.53 8.040.12 BD 1.14 22.47 8.70 2.23 BD BD 0.13 BD 4.10 4.82 BD BD0.08 3.28 0.17 0.06 1.45 0.04 0.01 0.09 0.03 0.01 0.03 0.01 0.01 0.01

29.00 7.60 4.16 10.82 9.72 16.00 4.62 4.37BD BD 0.65 0.66 BD BD BD BD BD BD 0.16 0.14 BD BD

0.09 2.60 0.14 0.08 1.23 0.09 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.0110.38 11.43 11.44 10.66

BD BD 0.76 0.86 BD 0.21 BD BD BD BD 0.15 0.17 BD BD

335

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95DL 0.46 0.77 0.48 21.87 0.09 0.18 0.67 0.42 0.48 2.83 0.02 0.55Precision(%) 7.01 3.78 4.97 15.07 84.05 29.64 7.73 6.65

Golden Mile Chron. Samples Fimiston Stage I UG1_1-1 Conc. (ppm) 8.46 BD 164.46 465000.00 555.95 38.24 1054.28 9.44 612.71 25.18 BD 13.80DL 0.39 0.64 0.70 6.15 0.06 0.14 0.76 0.32 0.63 4.73 0.02 0.51Precision(%) 6.71 9.77 3.64 6.96 9.10 10.31 6.85 8.32 8.70 11.70



Golden Mile Chron. Samples Fimiston Stage II 233-1-1 Conc. (ppm) 10.88 BD 59.44 465000.00 323.82 70.54 142.86 6.73 990.28 12.61 0.39 1.13DL 0.44 0.74 0.57 6.95 0.06 0.17 0.75 0.43 0.58 3.34 0.01 0.55Precision(%) 5.40 4.43 3.37 4.35 4.16 11.38 8.08 3.43 12.53 25.86 20.47



Golden Mile Chron. Samples Fimiston Stage II 233-3-1 Conc. (ppm) 293.00 5.56 27.56 465000.00 1033.94 199.17 229.75 16.68 721.58 21.38 169.19 0.62DL 0.68 0.80 0.54 16.35 0.07 0.19 0.96 0.50 0.60 3.31 0.02 0.57Precision(%) 11.76 10.77 14.75 3.35 5.27 4.61 9.93 15.14 3.69 7.97 5.69 38.78

Golden Mile Chron. Samples Fimiston Stage II 233-4-1 Conc. (ppm) 352.21 1.93 16.80 465000.00 1545.42 387.43 101.57 19.03 1401.55 19.83 9.32 2.04DL 0.41 0.60 0.66 17.51 0.05 0.07 0.79 0.39 0.70 3.99 0.02 0.54Precision(%) 12.18 18.01 15.61 3.40 3.11 4.44 8.69 5.26 3.88 9.50 8.76 19.96

Golden Mile Chron. Samples Fimiston Stage II 3766_1 Conc. (ppm) 6.89 BD 0.58 465000.00 558.76 806.69 BD 0.72 39.49 14.94 BD BDDL 0.42 0.83 0.38 6.79 0.03 0.12 0.47 0.24 2.21 4.86 0.02 0.54Precision(%) 6.82 27.40 3.46 4.15 4.21 19.33 5.10 14.70

Golden Mile Chron. Samples Fimiston Stage II 3766_2 Conc. (ppm) 504.36 1.50 0.44 465000.00 212.43 561.98 29.41 1.06 26.83 13.55 9.57 BDDL 0.39 0.56 0.37 6.05 0.03 0.15 0.52 0.24 2.77 3.43 0.02 0.72Precision(%) 17.49 23.71 35.21 3.49 9.33 11.93 13.49 16.23 5.48 12.43 10.63

Golden Mile Chron. Samples Fimiston Stage II 3766_3 Conc. (ppm) 269.60 18.82 447.13 465000.00 298.90 796.24 21.78 29.63 111.77 15.39 28.36 3.20DL 0.60 0.89 0.52 7.70 0.06 0.16 0.47 0.30 3.43 4.63 0.02 0.77Precision(%) 16.54 11.84 11.23 5.56 5.61 6.98 17.65 10.04 9.46 14.53 7.52 18.12

Golden Mile Chron. Samples Fimiston Stage II 3766_4 Conc. (ppm) 123.24 41.15 107.99 465000.00 98.81 361.18 117.12 12.62 63.28 8.70 13.72 2.98DL 0.54 0.66 0.46 19.90 0.04 0.11 0.49 0.33 2.90 4.73 0.02 0.69Precision(%) 9.73 10.34 16.59 4.52 7.21 5.16 18.54 10.69 5.70 22.87 13.48 18.10

Golden Mile Chron. Samples Fimiston Stage II 52280_1-1 Conc. (ppm) 1044.19 BD BD 465000.00 17.81 7.44 24.38 2.34 9033.48 14.44 5.08 0.64DL 0.64 0.73 0.62 9.29 0.05 0.22 0.70 0.43 0.44 3.64 0.02 0.58Precision(%) 27.51 3.77 13.09 7.13 8.31 18.20 6.41 11.30 28.25 38.57

Golden Mile Chron. Samples Fimiston Stage II 52280_1-2 Conc. (ppm) 9.12 BD 475.76 465000.00 12.45 7.93 52.23 22.80 7847.98 15.97 0.06 0.48DL 0.51 0.74 0.48 20.07 0.04 0.18 0.68 0.42 0.93 3.62 0.03 0.44Precision(%) 7.39 16.63 2.50 5.80 5.99 7.03 12.09 3.65 10.53 38.06 37.97

Golden Mile Chron. Samples Fimiston Stage II 52280_2-1 Conc. (ppm) 6.42 BD 24.09 465000.00 1.84 2.30 41.01 2.02 24235.20 13.60 BD BDDL 1.20 0.73 0.61 7.31 0.04 0.08 0.75 0.41 0.61 3.21 0.02 0.51Precision(%) 9.31 14.07 3.62 14.60 8.06 5.40 15.16 3.77 12.10

Golden Mile Chron. Samples Fimiston Stage II 52280_2-3 Conc. (ppm) 17.78 BD 410.67 465000.00 2.27 1.64 18.31 7.10 15975.14 17.43 1.10 BDDL 0.91 1.21 1.17 14.38 0.10 0.31 1.39 0.75 1.38 6.74 0.03 0.95Precision(%) 7.02 11.45 3.88 7.33 15.24 6.56 14.10 4.01 17.60 12.38

Golden Mile Chron. Samples Fimiston Stage II 52299_1-1 Conc. (ppm) 647.71 119.03 44.87 465000.00 31.99 153.33 2.78 6.69 44.94 BD 24.21 BDDL 0.59 0.73 0.52 14.97 0.08 0.20 0.85 0.38 0.63 3.59 0.01 0.53

336


UG1_1-1 Conc. (ppm)DLPrecision(%)



233-1-1 Conc. (ppm)DLPrecision(%)













52299_1-1 Conc. (ppm)DL


8.92 10.66 29.76 11.55 13.073.59 BD 0.85 15.90 5.06 4.59 0.02 0.03 0.48 0.07 64.04 21.22 BD BD0.10 2.89 0.14 0.05 1.31 0.09 0.01 0.02 0.03 0.01 0.02 0.01 0.01 0.006.71 8.86 7.51 12.78 10.75 28.31 39.20 10.23 14.82 7.52 7.19

11.32 BD 1.40 5.92 BD 24.64 0.05 BD 3.27 0.05 36.07 8.73 BD BD0.20 4.56 0.23 0.13 2.60 0.11 0.01 0.08 0.02 0.02 0.04 0.02 0.01 0.01

12.56 11.78 13.41 14.22 41.56 13.44 23.74 13.09 12.99 131.9618.96 BD 1.14 39.35 10.12 0.54 BD 0.16 1.19 0.19 84.48 22.08 BD BD0.08 2.99 0.16 0.08 1.10 0.06 0.01 0.03 0.04 0.01 0.03 0.02 0.00 0.01

17.43 7.70 20.14 17.02 25.06 51.74 32.30 8.22 3.44 3.160.39 BD 0.82 24.39 BD 8.82 0.06 BD 0.04 2.14 85.61 0.42 BD BD0.11 2.41 0.12 0.09 1.39 0.10 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.01

14.57 7.83 3.67 24.17 19.11 37.23 4.04 3.93 5.490.37 BD 0.85 20.13 2.03 1.18 0.81 1.44 0.09 0.29 72.25 0.87 0.03 0.020.09 2.49 0.14 0.08 1.32 0.07 0.01 0.03 0.03 0.02 0.03 0.02 0.01 0.01

14.70 8.53 7.98 29.37 10.12 10.69 15.03 21.00 7.45 4.01 4.40 22.68 21.721.06 BD 0.90 36.58 2.03 1.58 0.50 0.14 0.11 1.43 101.44 1.99 BD BD0.15 2.49 0.13 0.08 1.57 0.12 0.01 0.03 0.02 0.02 0.04 0.01 0.01 0.018.72 7.90 3.18 32.49 38.10 20.73 16.09 17.51 3.63 2.74 3.711.00 3.03 0.94 40.32 2.26 54.64 3.88 0.40 0.16 0.47 106.39 2.42 3.44 0.500.08 2.96 0.15 0.08 1.65 0.12 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.018.55 38.35 7.64 3.89 31.13 7.21 7.97 21.84 13.56 5.40 3.39 3.96 4.44 4.640.92 BD 0.83 59.95 2.02 8.67 0.47 0.43 0.16 1.05 246.42 2.54 0.14 0.040.13 3.21 0.15 0.08 1.63 0.09 0.01 0.04 0.05 0.02 0.03 0.01 0.01 0.019.36 9.00 3.53 33.48 11.73 14.84 12.37 16.37 5.61 4.39 3.72 8.37 13.89

BD BD 0.45 BD BD BD BD BD BD BD BD BD BD BD0.10 3.15 0.14 0.06 1.38 0.06 0.01 0.06 0.05 0.01 0.03 0.01 0.01 0.01

13.531.72 BD 0.49 0.99 2.54 BD 0.41 2.89 0.87 BD 2.05 0.09 0.43 0.130.11 2.95 0.14 0.06 1.56 0.13 0.01 0.05 0.03 0.01 0.03 0.02 0.01 0.01

16.05 13.14 9.87 28.44 40.33 17.33 16.11 7.31 15.23 10.40 10.573.29 BD 0.85 7.13 14.55 27.70 0.59 3.08 0.58 0.14 39.27 1.72 0.61 0.390.11 3.22 0.15 0.08 1.89 0.12 0.01 0.06 0.04 0.01 0.04 0.01 0.01 0.01

15.49 9.06 5.43 14.54 12.39 12.98 19.04 13.86 14.04 10.55 8.52 7.82 9.013.91 BD 0.88 6.68 12.32 61.90 0.12 0.66 BD 0.17 23.06 0.71 0.32 0.190.09 2.49 0.17 0.09 1.35 0.08 0.01 0.03 0.07 0.02 0.04 0.02 0.01 0.01

18.66 9.88 10.61 10.27 10.63 20.24 12.99 11.71 7.65 7.57 12.34 14.590.21 BD 0.81 17.68 5.17 0.29 0.12 11.46 12.32 0.40 3.19 0.03 BD BD0.11 2.58 0.16 0.08 0.99 0.09 0.01 0.03 0.05 0.01 0.03 0.01 0.01 0.01

27.01 9.03 7.93 13.68 26.08 27.91 26.71 9.32 12.01 8.43 27.850.39 BD 0.78 12.14 4.42 0.44 0.05 0.05 28.44 0.21 5.42 0.26 BD BD0.08 2.84 0.15 0.09 1.28 0.05 0.01 0.04 0.01 0.02 0.03 0.01 0.01 0.01

14.62 182.33 9.19 9.58 15.48 19.07 22.69 36.49 6.93 15.78 4.83 7.680.21 BD 0.70 3.90 1.25 BD BD BD 26.60 0.09 0.90 0.05 BD BD0.09 3.00 0.16 0.06 0.82 0.06 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.00

21.84 10.29 9.34 32.92 7.63 15.02 11.67 23.40BD BD 1.01 3.01 BD 0.39 0.25 0.69 40.48 0.05 0.53 BD BD BD

0.16 4.71 0.27 0.15 2.16 0.15 0.02 0.08 0.05 0.02 0.05 0.02 0.01 0.0112.28 10.80 24.12 18.25 19.33 6.65 21.67 12.26

BD BD 1.21 1.94 38.89 0.16 0.09 38.02 0.06 BD 3.06 BD 0.31 0.160.13 2.45 0.13 0.07 1.62 0.08 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.01

337

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Precision(%) 15.02 21.93 16.65 3.89 7.27 6.63 18.40 17.65 5.89 10.88

Golden Mile Chron. Samples Fimiston Stage II 52299_1-2 Conc. (ppm) 25.50 14.22 24.62 465000.00 130.19 146.61 650.38 41.76 213.35 3.92 80.85 BDDL 0.59 0.73 0.55 13.50 0.05 0.24 0.81 0.42 0.48 3.52 0.02 0.48Precision(%) 12.50 8.70 6.71 3.42 4.09 3.94 13.73 8.24 8.47 37.24 9.41


Golden Mile Chron. Samples Fimiston Stage II 52299_2-2 Conc. (ppm) 13.39 11.09 21.11 465000.00 203.01 284.18 171.97 16.77 129.44 BD 1.79 BDDL 0.55 0.77 0.59 28.45 0.08 0.25 0.64 0.66 0.61 3.07 0.01 0.54Precision(%) 9.41 10.20 8.44 3.45 11.53 7.97 10.27 12.38 10.76 10.95

Golden Mile Chron. Samples Fimiston Stage II 52299_3-1 Conc. (ppm) 10.17 BD BD 465000.00 235.49 534.50 BD 0.82 273.36 16.00 20.59 BDDL 0.31 0.87 0.60 8.55 0.06 0.14 0.88 0.32 0.60 3.55 0.02 0.58Precision(%) 20.04 3.85 5.16 3.98 21.57 3.98 11.14 21.39

Golden Mile Chron. Samples Fimiston Stage II 52299_3-2 Conc. (ppm) 17.21 2.98 3.78 465000.00 86.59 133.50 263.34 5.49 447.72 BD 2.96 BDDL 0.49 0.63 0.51 13.55 0.07 0.23 0.76 0.31 0.64 4.28 0.01 0.50Precision(%) 22.87 13.59 12.03 3.92 4.64 4.70 12.93 8.70 6.61 10.72

Golden Mile Chron. Samples Fimiston Stage II 52299_4-1 Conc. (ppm) 46.47 1.17 1.07 465000.00 99.07 59.07 54.99 3.21 110.21 BD 48.81 0.57DL 0.40 0.66 0.52 8.54 0.06 0.15 0.81 0.31 0.57 3.81 0.01 0.49Precision(%) 12.40 26.78 20.85 3.74 7.52 4.46 17.60 10.95 5.68 12.38 37.57


Golden Mile Chron. Samples Fimiston Stage III 52198_1 Conc. (ppm) 108.54 0.88 1.16 465000.00 100.46 487.33 2.29 1.33 178.06 6.37 7.73 BDDL 0.29 0.82 0.50 7.72 0.04 0.14 0.52 0.33 2.37 4.22 0.01 0.57Precision(%) 16.45 40.41 21.81 3.78 7.64 5.01 24.57 14.14 15.03 28.76 38.37

Golden Mile Chron. Samples Fimiston Stage III 52198_2 Conc. (ppm) 10.09 BD 7.09 465000.00 358.42 188.55 372.88 25.02 143.64 14.80 0.04 BDDL 0.40 0.78 0.46 17.38 0.06 0.21 0.46 0.30 2.51 3.08 0.01 0.58Precision(%) 6.01 9.92 3.58 4.37 5.37 15.58 40.51 6.31 12.53 40.15



Golden Mile Chron. Samples Fimiston Stage III LGX_2-1 Conc. (ppm) 20.25 BD 0.83 465000.00 58.74 3.97 2.27 0.92 35.06 39.15 28.97 BDDL 0.40 0.61 0.34 12.03 0.05 0.13 0.52 0.23 1.93 4.59 0.01 0.67Precision(%) 12.25 27.91 3.62 8.22 5.99 14.26 16.47 6.30 6.97 9.67

Golden Mile Chron. Samples Fimiston Stage III LGX_2-2 Conc. (ppm) 54674.46 BD 84.02 465000.00 68.89 4.83 151.37 14.14 769.45 9.84 56.01 0.79DL 0.44 0.74 0.33 8.32 0.04 0.09 0.53 0.34 1.94 5.79 0.02 0.63Precision(%) 10.96 14.10 4.02 3.99 7.01 15.79 14.32 6.50 24.47 6.85 32.78

Golden Mile Chron. Samples Fimiston Stage III LGX_2-3 Conc. (ppm) 691.96 BD 51.38 465000.00 81.51 6.38 24.99 325.52 295.94 27.12 52.05 BDDL 0.67 0.63 0.31 9.34 0.04 0.17 0.44 0.18 1.51 4.20 0.01 0.61Precision(%) 7.93 21.27 2.88 6.55 6.39 6.69 43.10 10.37 8.98 8.75

Golden Mile Chron. Samples Fimiston Stage III LGX_5-1 Conc. (ppm) 6.99 0.17 BD 465000.00 5.16 11.47 BD 0.62 55.66 27.48 BD BDDL 0.26 0.81 0.34 5.17 0.04 0.15 0.43 0.20 1.70 5.30 0.01 0.48Precision(%) 5.76 177.40 3.74 7.96 7.85 19.02 4.68 9.78

Golden Mile Chron. Samples Fimiston Stage III LGX_5-2 Conc. (ppm) 6.18 BD BD 465000.00 116.29 21.34 0.64 0.87 39.65 31.00 BD BDDL 0.43 0.75 0.35 4.51 0.02 0.14 0.50 0.20 1.70 5.12 0.01 0.63Precision(%) 6.21 3.69 10.55 10.32 42.43 15.89 9.70 9.67

Golden Mile Chron. Samples Fimiston Stage III UG10_1 Conc. (ppm) 16487.61 2.37 23.91 465000.00 250.88 250.99 296.66 3.29 1448.66 9.03 14.45 BDDL 0.45 0.76 0.44 8.14 0.05 0.21 0.46 0.38 2.39 4.86 0.02 0.70Precision(%) 17.67 22.06 17.92 4.98 9.87 9.46 17.92 13.54 7.82 23.64 12.34

338













LGX_2-1 Conc. (ppm)DLPrecision(%)





UG10_1 Conc. (ppm)DLPrecision(%)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2388.83 8.26 6.07 31.87 15.93 15.32 29.13 7.34 11.17 10.02

65.34 BD 0.87 6.32 76.39 0.16 11.75 0.13 14.54 0.05 47.34 0.54 2.27 0.580.10 2.81 0.12 0.09 1.28 0.10 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.01

16.29 8.03 5.09 18.87 31.59 30.38 18.90 24.14 16.70 5.52 7.24 11.62 9.844.79 BD 0.77 1.29 9.97 0.20 BD BD 1.08 0.03 4.89 0.10 0.09 0.050.13 2.54 0.16 0.09 1.05 0.07 0.01 0.05 0.04 0.01 0.04 0.01 0.01 0.01

10.99 9.83 8.89 10.35 26.56 10.84 32.63 7.97 13.63 11.75 12.651.15 BD 0.82 5.92 BD 0.15 0.03 BD 0.12 0.09 60.33 0.33 0.04 BD0.11 2.19 0.15 0.08 1.47 0.10 0.01 0.06 0.04 0.01 0.04 0.02 0.01 0.01

11.47 8.90 6.90 41.11 44.70 20.65 12.27 7.13 8.37 18.64BD BD 0.86 0.13 BD 0.23 BD 0.07 BD BD 0.28 BD 0.15 0.16

0.10 2.83 0.17 0.08 1.64 0.09 0.01 0.03 0.03 0.01 0.02 0.01 0.01 0.019.45 31.90 51.40 34.85 17.80 21.72 21.75

23.19 BD 0.91 12.47 25.75 BD BD 0.13 3.12 0.04 112.08 0.84 0.03 0.020.10 3.03 0.15 0.08 1.36 0.12 0.01 0.04 0.03 0.02 0.02 0.01 0.00 0.00

14.63 8.33 8.77 12.18 39.60 14.63 20.59 9.10 8.45 20.73 15.896.90 BD 0.85 2.53 11.45 BD 0.24 0.16 1.75 0.02 16.40 0.29 1.30 0.370.08 2.46 0.16 0.08 1.43 0.10 0.01 0.04 0.03 0.01 0.02 0.01 0.01 0.00

12.71 8.59 6.54 11.63 27.82 25.74 13.09 34.03 5.17 6.84 12.01 12.402.62 3.59 2.99 2.95 5.68 5.67 0.73 0.68 0.62 0.05 16.12 0.06 0.47 0.220.15 3.20 0.24 0.07 2.62 0.12 0.02 0.08 0.06 0.01 0.05 0.01 0.01 0.01

13.67 41.40 9.63 11.26 21.22 15.31 27.41 19.43 17.05 19.77 10.36 17.31 13.02 15.820.15 BD 0.55 0.46 2.42 0.13 BD 0.65 0.29 0.02 1.02 BD 0.02 0.020.09 2.44 0.13 0.05 1.12 0.08 0.01 0.03 0.06 0.01 0.03 0.01 0.01 0.01

31.05 11.81 16.74 24.07 34.17 15.82 19.26 32.64 13.18 42.99 51.5827.82 3.42 0.59 5.99 61.98 0.41 BD BD 8.84 0.31 14.38 0.25 0.01 BD0.10 3.14 0.16 0.06 1.29 0.08 0.01 0.04 0.03 0.01 0.03 0.01 0.00 0.01

39.79 36.24 12.10 6.78 8.70 20.82 38.81 7.52 4.34 6.95 38.931.32 BD 0.70 8.13 8.63 1.17 0.29 9.91 1.71 0.18 8.36 0.02 BD 0.020.10 3.13 0.12 0.06 1.14 0.00 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.019.58 9.47 10.83 13.60 22.22 10.13 9.80 16.43 17.67 8.95 28.66 26.96

25.27 BD 4.96 13.48 55.57 0.31 0.15 3.46 52.68 0.14 9.11 0.08 BD 0.020.11 2.39 0.15 0.04 1.62 0.08 0.01 0.05 0.04 0.02 0.02 0.02 0.01 0.01

14.69 86.56 21.86 9.43 25.16 10.68 10.64 13.60 10.94 4.22 14.41 28.344.19 BD 0.54 0.15 6.46 0.27 BD BD 2.39 BD 0.64 BD 0.02 0.040.09 2.61 0.12 0.07 1.33 0.06 0.01 0.03 0.04 0.02 0.02 0.01 0.01 0.01

17.95 10.59 24.69 15.75 21.53 22.13 13.45 22.25 16.2529.07 BD 19.12 195.19 55.81 7.90 4.94 168.05 18.91 0.61 11.10 BD 0.52 0.620.10 2.78 0.12 0.08 1.07 0.07 0.01 0.04 0.03 0.01 0.03 0.02 0.01 0.01

15.37 10.40 9.17 9.05 11.09 10.01 10.00 9.98 7.59 3.86 9.77 10.4570.22 BD 0.92 9.98 254.49 10.56 7.47 5.37 8.53 0.48 8.77 BD 0.10 0.120.07 2.13 0.10 0.06 1.19 0.08 0.01 0.03 0.05 0.02 0.02 0.01 0.01 0.01

11.36 7.59 8.66 29.21 20.03 58.82 11.37 14.72 12.56 6.29 19.79 11.19BD 2.63 0.43 BD BD BD BD BD BD BD BD BD BD BD

0.09 2.45 0.11 0.07 1.09 0.05 0.01 0.02 0.03 0.01 0.02 0.01 0.00 0.0137.13 12.02

0.09 BD 0.49 BD BD BD BD BD 0.03 BD 0.04 BD BD BD0.07 2.56 0.13 0.06 1.59 0.08 0.01 0.03 0.01 0.02 0.02 0.01 0.01 0.01

52.64 20.20 32.09 30.336.66 BD 1.16 42.43 47.26 19.52 0.61 88.43 7.96 0.22 24.26 0.13 0.42 0.600.12 2.73 0.16 0.07 1.10 0.09 0.01 0.05 0.05 0.01 0.03 0.02 0.01 0.01

10.50 9.82 14.25 9.20 20.24 15.35 16.60 11.13 16.50 6.86 11.74 16.51 16.19

339

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Golden Mile Chron. Samples Fimiston Stage III UG10_2 Conc. (ppm) 4986.75 82.11 2785.45 465000.00 280.95 266.19 2604.59 159.59 1109.71 7.09 7.21 BD

DL 0.79 1.00 0.97 11.60 0.11 0.29 0.89 0.45 3.95 6.28 0.04 1.05Precision(%) 11.16 11.88 12.47 12.85 16.28 15.27 27.18 13.26 16.09 40.17 19.34



Golden Mile Chron. Samples Fimiston Stage III UG10_5 Conc. (ppm) 12274.80 2.54 0.78 465000.00 105.42 45.75 53.00 54.72 3327.74 6.73 126.25 0.80DL 0.55 0.77 0.54 12.54 0.05 0.14 0.55 0.37 2.70 3.97 0.02 0.69Precision(%) 12.33 19.80 29.67 5.92 7.30 6.09 8.27 33.10 7.74 26.47 17.94 37.75

Golden Mile Chron. Samples Fimiston Stage IV UG3_1-1 Conc. (ppm) 213.32 2.65 1.09 465000.00 124.20 79.29 15272.72 2847.44 4253.88 12.02 8.79 4.62DL 0.56 0.75 0.63 8.43 0.05 0.22 0.72 0.45 0.89 3.22 0.02 0.63Precision(%) 21.95 17.38 30.14 3.77 10.84 8.43 12.87 12.65 10.17 13.95 10.00 22.60

Golden Mile Chron. Samples Fimiston Stage IV UG3_1-2 Conc. (ppm) 111.30 2.51 0.78 465000.00 104.17 62.81 1368.74 135.50 7905.87 5.29 7.02 1.26DL 0.48 0.67 0.44 5.52 0.04 0.18 0.77 0.47 0.62 2.61 0.01 0.40Precision(%) 14.61 16.95 33.13 4.35 5.34 6.34 6.48 9.59 8.25 22.30 7.29 16.20

Golden Mile Chron. Samples Fimiston Stage IV UG3_2-1 Conc. (ppm) 22.64 0.71 43.58 465000.00 265.14 164.94 1626.91 130.93 14781.50 BD 0.85 BDDL 0.48 0.69 0.70 9.42 0.06 0.20 0.84 0.32 0.56 3.25 0.01 0.59Precision(%) 47.01 42.68 11.75 3.68 4.36 4.31 7.84 7.08 4.04 35.01

Golden Mile Chron. Samples Fimiston Stage IV UG3_3-1 Conc. (ppm) 8.61 BD 1.18 465000.00 243.26 141.94 1885.90 279.51 9220.80 3.83 0.07 BDDL 0.37 0.75 0.49 6.85 0.04 0.22 0.72 0.26 0.50 3.12 0.01 0.53Precision(%) 9.92 41.70 4.16 4.68 4.45 6.47 4.37 5.36 32.29 22.94

Golden Mile Fimiston Aberdare ABD10_1 Conc. (ppm) 675.61 12.73 523.23 465000.00 89.43 112.78 13.39 22.09 42.19 BD 5.02 BDDL 0.28 0.90 0.42 7.09 0.05 0.14 0.64 0.42 2.21 4.87 0.01 0.62Precision(%) 19.27 9.03 8.61 3.86 6.19 5.88 7.37 7.81 4.69 19.51

Golden Mile Fimiston Aberdare ABD10_2C Conc. (ppm) 736.13 6.31 717.41 465000.00 89.84 114.67 5.34 31.01 42.41 BD 5.04 BDDL 0.55 0.55 0.48 9.61 0.04 0.16 0.60 0.44 2.06 5.01 0.02 0.59Precision(%) 18.17 9.58 8.94 3.34 5.49 4.21 8.15 7.97 5.55 28.53

Golden Mile Fimiston Aberdare ABD10_2R Conc. (ppm) 43.03 BD 4.91 465000.00 854.00 162.00 BD 0.68 267.74 33.31 0.05 BDDL 0.53 0.73 0.41 9.43 0.05 0.16 0.62 0.43 2.06 4.38 0.02 0.69Precision(%) 15.28 27.10 4.07 7.55 3.78 29.47 4.14 7.50 25.35

Golden Mile Fimiston Aberdare ABD10_3C Conc. (ppm) 269.44 BD 386.07 465000.00 332.58 286.49 4.23 15.30 132.28 11.26 4.11 BDDL 0.60 0.80 0.42 15.38 0.05 0.12 0.62 0.31 1.59 5.21 0.02 0.72Precision(%) 26.99 12.91 3.79 10.36 4.67 13.92 11.40 7.78 21.99 68.85

Golden Mile Fimiston Aberdare ABD10_3R Conc. (ppm) 7.73 BD 100.91 465000.00 341.77 305.59 1.57 8.57 137.74 46.88 0.01 BDDL 0.48 0.70 0.50 9.53 0.04 0.19 0.56 0.47 1.80 4.55 0.02 0.65Precision(%) 7.46 13.69 4.27 9.88 9.74 19.01 12.77 6.82 6.72 71.77

Golden Mile Fimiston Aberdare ABD15_1 Conc. (ppm) 10.60 BD 0.79 465000.00 3517.69 5226.82 78.36 4.63 3017.05 BD 0.09 BDDL 0.37 0.55 0.33 5.68 0.03 0.12 0.47 0.28 1.43 5.34 0.02 0.61Precision(%) 15.68 18.69 4.16 5.00 5.37 7.82 7.95 5.64 30.14

Golden Mile Fimiston Aberdare ABD15_2 Conc. (ppm) 9.14 0.37 2.02 465000.00 3649.08 5045.15 144.62 9.69 8048.50 11.02 0.43 0.61DL 0.33 0.51 0.42 4.82 0.04 0.15 0.62 0.25 1.80 4.53 0.02 0.55Precision(%) 6.16 60.14 11.05 4.04 4.33 4.61 10.12 21.02 7.59 17.35 69.35 37.15

Golden Mile Fimiston Aberdare ABD15_3 Conc. (ppm) 1292.11 1.55 35.97 465000.00 5212.95 2713.07 2602.59 15.26 9866.02 43.09 15.10 0.51DL 0.47 0.68 0.49 7.87 0.06 0.15 0.66 0.24 1.89 5.55 0.02 0.66Precision(%) 10.67 22.20 11.38 4.30 4.71 4.44 9.34 6.82 4.58 7.24 15.83 54.19

Golden Mile Fimiston Aberdare ABD15_4 Conc. (ppm) 238.89 27.86 107.29 465000.00 4693.78 896.31 4084.41 19.31 6518.16 40.00 57.18 BDDL 1.16 1.33 0.58 16.71 0.12 0.48 1.15 0.53 3.48 8.78 0.05 1.51Precision(%) 10.15 11.54 26.20 12.39 12.34 12.09 27.12 13.48 11.94 14.67 25.27

340

Sample NoUG10_2 Conc. (ppm)

DLPrecision(%)








ABD10_1 Conc. (ppm)DLPrecision(%)

ABD10_2C Conc. (ppm)DLPrecision(%)

ABD10_2R Conc. (ppm)DLPrecision(%)

ABD10_3C Conc. (ppm)DLPrecision(%)

ABD10_3R Conc. (ppm)DLPrecision(%)





Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23816.12 BD 3.20 27.60 49.11 134.56 1.88 40.73 25.32 1.37 29.68 0.16 0.06 0.070.15 4.93 0.34 0.10 2.33 0.15 0.01 0.12 0.06 0.02 0.07 0.02 0.01 0.02

27.45 10.78 14.60 26.61 16.76 11.20 10.57 62.16 15.82 12.21 19.79 19.39 27.9412.15 BD 1.30 15.43 212.17 0.18 0.14 2.89 13.14 0.72 44.85 0.26 BD BD0.08 2.53 0.14 0.06 1.26 0.08 0.01 0.05 0.05 0.02 0.03 0.01 0.01 0.015.97 8.05 4.24 6.66 25.77 10.54 9.26 7.89 5.42 3.33 6.074.47 BD 1.21 5.73 30.54 42.68 0.05 0.81 7.35 0.22 16.38 0.20 BD BD0.11 3.30 0.16 0.09 1.36 0.08 0.01 0.03 0.05 0.01 0.02 0.01 0.01 0.018.40 14.49 6.94 8.64 13.99 15.27 16.20 9.35 8.71 5.75 9.525.79 BD 1.37 36.90 55.35 53.24 0.53 76.14 10.05 0.31 34.76 0.26 0.56 0.770.09 3.34 0.17 0.09 1.67 0.11 0.01 0.04 0.05 0.02 0.03 0.01 0.01 0.01

10.49 9.01 8.52 8.51 17.87 12.73 12.19 8.51 11.30 7.60 9.18 12.83 12.933.63 22.05 1.33 5741.31 66.13 3.31 0.23 1.51 7.51 0.37 33.49 0.89 0.15 0.070.10 2.77 0.14 0.07 1.64 0.11 0.01 0.03 0.03 0.02 0.04 0.01 0.01 0.01

10.92 14.17 7.80 12.20 10.90 11.99 29.21 15.07 12.78 11.68 10.11 10.36 11.78 13.606.41 BD 1.84 76.56 12.35 3.73 0.19 0.51 22.16 0.34 52.78 0.27 0.39 0.190.08 2.29 0.14 0.11 1.04 0.08 0.01 0.04 0.03 0.01 0.04 0.01 0.00 0.018.11 7.70 8.20 9.41 9.86 13.25 11.85 37.07 7.42 7.23 7.45 6.93 8.407.26 BD 1.90 88.21 27.78 0.32 1.18 0.39 34.33 0.13 70.77 0.41 0.02 BD0.11 2.96 0.14 0.09 1.53 0.09 0.01 0.05 0.02 0.02 0.03 0.01 0.01 0.016.99 6.47 6.56 6.84 18.63 39.82 59.22 45.99 10.94 6.58 6.28 30.399.11 BD 3.44 153.59 16.74 BD BD BD 6.74 0.38 114.35 0.40 BD BD0.10 2.27 0.12 0.08 1.41 0.10 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.015.31 4.81 4.21 8.38 7.62 6.21 4.57 6.160.64 3.07 0.59 2.77 11.32 11.76 0.04 4.63 0.94 BD 20.79 0.08 BD BD0.10 2.71 0.13 0.06 1.61 0.05 0.01 0.08 0.06 0.02 0.04 0.01 0.01 0.01

12.05 36.55 11.80 6.10 10.42 8.61 14.52 21.58 12.91 4.36 13.660.23 BD 0.65 3.63 8.05 7.41 0.06 8.57 0.18 BD 20.08 0.05 BD BD0.08 3.66 0.17 0.09 1.80 0.09 0.01 0.05 0.07 0.01 0.03 0.02 0.02 0.01

19.76 12.35 8.06 11.93 6.25 14.78 20.97 23.23 4.08 21.13 1825.620.04 BD 0.46 0.35 BD 0.33 BD 0.49 BD BD 0.71 BD BD BD0.09 3.38 0.16 0.08 1.79 0.09 0.01 0.04 0.05 0.02 0.02 0.01 0.01 0.01

102.21 15.31 19.42 20.63 23.79 12.710.38 3.27 0.53 3.68 6.14 3.32 0.02 1.78 0.39 BD 24.74 0.02 BD BD0.11 3.25 0.17 0.07 1.68 0.10 0.01 0.06 0.06 0.02 0.03 0.01 0.01 0.01

21.66 40.56 14.17 10.34 16.78 20.97 21.52 19.62 18.14 12.83 31.59 745.40

BD BD 0.55 1.64 BD 0.68 BD BD 0.24 BD 2.72 BD BD BD0.12 3.55 0.13 0.06 1.61 0.09 0.01 0.04 0.05 0.02 0.03 0.02 0.01 0.01

11.38 15.34 27.42 20.74 8.931.34 BD 0.53 29.30 7.82 1.42 BD 0.04 0.95 32.85 30.41 1.12 BD BD0.08 2.50 0.15 0.07 1.59 0.06 0.01 0.03 0.05 0.01 0.02 0.01 0.01 0.018.76 12.52 4.45 11.27 21.93 47.01 9.55 4.76 5.09 6.00 98.011.83 BD 0.50 31.60 8.04 1.25 BD BD 1.12 23.44 45.86 1.37 BD BD0.08 2.88 0.14 0.05 1.20 0.08 0.01 0.04 0.05 0.01 0.03 0.01 0.01 0.016.49 12.68 4.23 9.65 11.39 7.77 4.35 4.87 5.216.76 BD 0.70 120.33 19.60 8.84 0.07 2.72 2.61 4.48 149.67 4.50 0.02 BD0.10 3.76 0.12 0.07 1.42 0.08 0.01 0.07 0.04 0.01 0.02 0.02 0.01 0.015.03 10.07 5.65 7.49 8.25 27.58 10.71 7.65 5.47 5.20 4.76 27.263.46 BD 2.12 102.54 4.61 281.30 BD 1.03 0.91 2.27 59.92 1.46 0.03 BD0.21 6.49 0.28 0.16 2.94 0.17 0.02 0.08 0.11 0.03 0.06 0.03 0.02 0.02

13.13 11.84 11.21 28.79 10.65 14.95 15.67 10.20 12.14 11.35 47.48

341

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Golden Mile Fimiston Aberdare ADGD1/12_1-1 Conc. (ppm) 285.89 1.09 38.62 465000.00 50.22 46.44 13.77 4.21 5456.80 21.43 4.92 BD

DL 0.29 0.53 0.41 5.71 0.03 0.14 0.38 0.20 3.36 3.72 0.01 0.42Precision(%) 12.56 25.67 15.37 3.59 4.92 4.15 10.31 18.04 3.50 8.67 35.77

Golden Mile Fimiston Aberdare ADGD1/12_1-2 Conc. (ppm) 551.77 1.55 227.98 465000.00 77.47 42.03 23.81 14.94 6608.62 21.15 3.93 BDDL 0.38 0.40 0.25 5.07 0.03 0.14 0.47 0.30 3.57 3.67 0.02 0.42Precision(%) 25.39 21.70 28.55 3.75 7.42 8.47 32.30 15.87 4.23 8.80 22.07

Golden Mile Fimiston Aberdare ADGD1/12_1-5 Conc. (ppm) 42.80 BD 7.50 465000.00 164.05 91.66 23.02 82.89 1567.45 17.12 0.86 BDDL 0.25 0.51 0.27 16.52 0.04 0.17 0.42 0.24 1.96 4.09 0.01 0.37Precision(%) 5.36 13.35 3.44 7.75 7.14 9.50 4.80 7.16 13.50 11.76

Golden Mile Fimiston Aberdare ADGD1/12_2-1 Conc. (ppm) 7.13 BD 5.81 465000.00 92.15 21.52 328.61 2.54 75.67 4.89 BD BDDL 0.25 0.45 0.21 18.15 0.03 0.11 0.40 0.18 1.53 2.93 0.01 0.29Precision(%) 5.80 7.76 3.76 4.26 4.05 9.13 9.32 5.07 25.15


Golden Mile Fimiston Aberdare ADGD1/19_1 Conc. (ppm) 741.78 33.35 21.77 465000.00 457.84 328.35 498.33 63.41 75523.11 15.35 1.51 0.64DL 0.23 0.47 0.27 7.74 0.04 0.10 0.29 0.19 1.48 3.82 0.01 0.41Precision(%) 8.53 8.07 7.43 3.98 7.68 3.93 5.70 13.20 9.93 11.39 9.27 25.81




Golden Mile Fimiston Aberdare ADGD1/6_2-2 Conc. (ppm) 267.15 BD 140.65 465000.00 572.69 1111.63 1380.00 26.18 19106.76 BD 5.88 BDDL 0.42 0.55 0.32 11.87 0.03 0.15 0.46 0.21 2.34 4.09 0.01 0.56Precision(%) 12.76 10.10 3.08 5.08 5.82 9.40 8.01 4.68 9.22

Golden Mile Fimiston Aberdare ADGD1/6_2-3 Conc. (ppm) 93.69 BD 809.78 465000.00 967.16 1084.46 1592.14 64.59 10960.53 12.01 44.55 1.05DL 0.36 0.61 0.32 12.44 0.05 0.16 0.62 0.29 2.37 5.03 0.02 0.56Precision(%) 9.99 11.44 5.00 6.03 7.29 14.10 7.44 7.82 18.22 13.08 25.37

Golden Mile Fimiston Aberdare ADGD2/22_1 Conc. (ppm) 81.90 17.49 0.61 465000.00 371.78 16.84 1.36 2.37 399.31 BD 5.13 BDDL 0.58 0.82 0.51 6.98 0.05 0.22 0.64 0.21 2.11 6.09 0.01 0.86Precision(%) 10.73 12.40 32.40 9.51 11.42 9.94 23.97 10.97 9.69 22.97

Golden Mile Fimiston Aberdare ADGD2/22_2 Conc. (ppm) 7.59 BD BD 465000.00 5.31 4.15 BD 1.56 178.37 BD BD BDDL 0.30 0.53 0.36 4.78 0.04 0.14 0.46 0.24 1.22 3.91 0.01 0.38Precision(%) 5.34 3.22 10.52 9.82 15.74 5.65

Golden Mile Fimiston Aberdare ADGD2/22_3 Conc. (ppm) 16.21 1.73 BD 465000.00 131.49 31.69 1.15 1.63 643.14 6.25 4.50 BDDL 0.40 0.55 0.41 7.92 0.03 0.13 0.43 0.20 1.25 4.91 0.02 0.46Precision(%) 7.87 19.33 3.33 6.59 5.42 16.82 10.16 3.79 30.31 23.23

Golden Mile Fimiston Aberdare ADGD2/22_4 Conc. (ppm) 25.66 4.01 52.34 465000.00 1.97 14.50 1.42 12.58 18.91 BD 0.10 BDDL 0.37 0.58 0.35 6.40 0.05 0.11 0.42 0.36 1.48 4.65 0.01 0.59Precision(%) 7.84 14.30 7.70 4.49 5.66 6.36 14.99 9.36 10.66 34.20

Golden Mile Fimiston Aberdare ADGD2/3_1 Conc. (ppm) 1125.23 2.64 56.38 465000.00 3927.45 2200.93 503.61 40.11 2783.24 11.89 8.87 1.36DL 0.33 0.92 0.40 6.98 0.05 0.17 0.41 0.15 1.19 5.03 0.01 0.58Precision(%) 9.71 16.85 7.09 5.54 5.83 6.44 15.38 11.86 5.96 18.11 7.83 29.92


Golden Mile Fimiston Aberdare ADGD2/4_1-2 Conc. (ppm) 6253.17 104.06 23.06 465000.00 141.26 120.41 104.47 8.62 13580.58 19.98 8.29 BD

342

Sample NoADGD1/12_1-1 Conc. (ppm)

DLPrecision(%)

ADGD1/12_1-2 Conc. (ppm)DLPrecision(%)




ADGD1/19_1 Conc. (ppm)DLPrecision(%)












ADGD2/4_1-2 Conc. (ppm)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2380.36 BD 0.48 1.58 BD 0.18 0.07 0.57 BD BD 4.51 0.20 BD 0.010.05 2.21 0.09 0.04 1.14 0.05 0.00 0.04 0.03 0.01 0.02 0.01 0.00 0.00

11.03 9.02 7.81 44.29 15.68 12.37 4.40 7.51 44.63BD BD 0.73 1.43 BD 0.28 0.03 3.46 BD BD 4.49 0.09 BD BD

0.08 2.15 0.10 0.06 1.20 0.05 0.01 0.02 0.03 0.01 0.02 0.01 0.01 0.0110.57 15.16 24.12 25.51 28.54 11.85 15.17

0.51 BD 0.52 6.22 BD 0.09 0.01 0.82 0.04 BD 21.40 0.82 BD 0.010.08 2.09 0.08 0.04 1.32 0.05 0.00 0.04 0.02 0.01 0.02 0.01 0.01 0.00

14.24 8.70 7.42 35.21 29.06 8.84 30.21 8.05 8.38 29.130.42 BD 0.48 1.91 BD 0.16 BD BD BD 1.58 3.62 0.22 BD BD0.06 1.57 0.07 0.03 0.99 0.06 0.00 0.02 0.02 0.01 0.02 0.01 0.00 0.00

10.45 8.19 5.38 21.77 5.47 4.17 6.16BD BD 0.57 1.02 BD 0.92 0.05 0.18 BD BD 10.10 0.06 BD BD

0.10 2.62 0.10 0.06 1.34 0.06 0.01 0.02 0.05 0.01 0.02 0.01 0.01 0.019.28 12.92 34.58 29.42 25.97 16.69 15.77 76.56

5.86 BD 0.64 1754.56 BD 7.29 0.46 11.08 6.07 49.06 39.32 0.06 BD BD0.08 2.11 0.09 0.04 0.92 0.07 0.00 0.04 0.02 0.02 0.02 0.01 0.01 0.003.94 8.47 7.68 8.67 37.52 9.28 15.35 4.91 3.74 15.210.42 BD 0.58 51.26 4.77 18.25 BD 0.45 0.40 2.15 11.85 0.05 BD 0.040.07 2.60 0.10 0.06 1.10 0.04 0.01 0.04 0.03 0.01 0.02 0.01 0.01 0.00

16.29 9.58 12.00 16.07 20.43 43.66 10.29 18.74 8.73 17.28 16.390.52 0.90 0.65 350.01 2.31 1.01 0.11 6.81 5.32 24.16 31.67 0.02 0.03 0.020.11 2.67 0.10 0.07 1.11 0.08 0.01 0.03 0.03 0.01 0.01 0.01 0.00 0.01

12.68 113.28 8.53 8.22 23.12 13.91 16.21 6.01 6.23 8.75 8.18 24.31 15.46 21.740.90 BD 1.00 116.74 14.55 244.27 2.18 2.71 0.71 4.15 19.59 0.13 0.25 0.010.16 3.64 0.12 0.10 2.13 0.07 0.02 0.05 0.04 0.02 0.05 0.01 0.01 0.01

16.35 10.09 13.78 14.74 11.11 59.84 12.96 14.11 13.72 10.97 14.02 52.51 37.291.37 BD 0.49 311.57 24.72 2.39 0.13 0.50 1.23 17.32 24.61 0.13 0.06 BD0.05 2.27 0.10 0.04 1.05 0.07 0.01 0.03 0.03 0.01 0.02 0.01 0.01 0.017.66 10.17 3.73 5.99 7.68 18.16 13.48 6.28 4.08 3.78 7.66 11.791.93 BD 0.62 84.21 17.01 32.40 0.16 1.93 1.91 2.59 27.07 0.21 0.07 0.330.08 2.45 0.11 0.08 1.44 0.07 0.01 0.04 0.04 0.01 0.02 0.01 0.01 0.01

11.40 10.18 10.96 9.74 16.27 10.08 10.58 10.79 12.96 7.99 11.27 13.60 13.120.29 BD 0.99 9.70 BD 157.21 BD 0.52 0.16 0.48 9.92 0.87 BD BD0.10 3.43 0.14 0.09 1.84 0.13 0.01 0.04 0.05 0.02 0.04 0.02 0.01 0.01

23.69 11.46 7.92 12.03 13.69 25.58 11.73 9.39 8.79 94.69BD BD 0.53 BD BD BD BD BD BD BD 0.04 BD BD BD

0.06 2.14 0.10 0.04 1.12 0.06 0.00 0.03 0.02 0.01 0.02 0.01 0.01 0.0025.63 27.01

0.09 BD 0.57 5.59 1.22 20.59 BD 0.07 0.04 0.07 5.63 0.24 BD 0.010.07 3.03 0.09 0.06 1.01 0.06 0.00 0.03 0.03 0.01 0.02 0.01 0.01 0.00

37.69 9.28 7.42 38.93 12.87 27.66 35.89 14.26 11.32 10.13 40.82BD BD 0.61 12.49 1.84 32.87 BD 0.12 BD 0.21 19.57 0.33 BD BD

0.08 2.99 0.11 0.09 1.44 0.06 0.01 0.03 0.04 0.01 0.04 0.01 0.01 0.019.90 5.82 35.02 12.08 18.62 10.56 5.43 8.18

2.51 2.71 1.04 51.47 5.32 12.83 0.13 8.89 0.65 0.26 77.25 0.53 0.44 BD0.08 2.31 0.09 0.05 1.17 0.07 0.01 0.02 0.03 0.01 0.02 0.02 0.01 0.016.68 34.30 7.16 5.43 12.63 9.54 16.20 14.66 17.29 7.69 4.90 6.36 86.441.21 BD 0.50 116.99 0.90 4.97 BD 0.23 16.69 6.64 16.72 0.01 BD BD0.09 2.01 0.10 0.06 0.86 0.07 0.01 0.02 0.03 0.01 0.02 0.01 0.01 0.00

12.85 10.32 7.59 39.11 21.10 14.53 10.37 10.86 16.75 38.39 104.940.85 BD 1.40 97.43 BD 480.11 0.09 70.04 3.42 3.23 16.89 0.02 0.02 0.01

343

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95DL 0.74 0.89 0.64 13.15 0.08 0.26 0.81 0.43 3.75 8.65 0.02 1.01Precision(%) 15.00 12.10 13.04 14.25 13.64 13.83 21.99 12.04 14.36 23.08 14.14



Golden Mile Fimiston Depth D1_1-1 Conc. (ppm) 225.96 BD 46.41 465000.00 37.34 40.27 529.77 14.12 6458.27 BD 0.15 BDDL 0.43 0.79 0.60 7.59 0.05 0.13 0.60 0.32 4.92 4.51 0.02 0.47Precision(%) 21.82 19.61 4.00 4.74 6.90 14.00 22.54 5.06 19.03

Golden Mile Fimiston Depth D1_2-1 Conc. (ppm) 6.20 BD BD 465000.00 0.57 1.02 4.77 0.58 5366.79 BD BD BDDL 0.61 0.83 0.74 9.52 0.05 0.24 0.73 0.49 5.00 4.65 0.02 0.52Precision(%) 7.66 3.11 8.00 14.48 9.72 38.31 5.16



Golden Mile Fimiston Depth D1_5-1 Conc. (ppm) 932.92 BD 59.04 465000.00 364.19 90.32 51.59 6.46 465.32 20.67 8.24 BDDL 0.35 0.80 0.47 22.73 0.06 0.24 0.60 0.24 4.96 3.30 0.02 0.52Precision(%) 9.61 6.98 2.84 6.65 6.16 9.46 7.67 5.14 8.53 7.21

Golden Mile Fimiston Depth d12_4 Conc. (ppm) 168.15 1.60 23.15 465000.00 204.12 331.01 71.98 21.89 5616.35 6.22 1.19 BDDL 0.40 0.64 0.55 8.03 0.04 0.20 0.77 0.16 4.45 4.38 0.02 0.49Precision(%) 30.35 19.18 12.28 3.09 3.42 4.65 4.79 4.21 4.16 28.04 33.73

Golden Mile Fimiston Depth d12_5 Conc. (ppm) 41.91 BD 24723.05 465000.00 7.19 119.64 BD 449.53 178.15 BD BD BDDL 25.07 39.90 41.53 515.51 2.96 10.79 33.45 21.20 264.11 304.84 2.09 40.64Precision(%) 34.74 13.04 12.81 23.65 13.88 12.21 61.69

Golden Mile Fimiston Depth d12_5-2 Conc. (ppm) 64.78 3.40 145.97 465000.00 537.59 551.48 131.16 12.99 2730.20 11.54 3.61 BDDL 0.57 1.31 0.86 11.19 0.06 0.34 1.00 0.51 7.30 6.07 0.03 0.81Precision(%) 13.56 24.52 16.49 11.03 9.74 10.14 15.74 12.10 12.74 24.60 17.06

Golden Mile Fimiston Depth D12-1 Conc. (ppm) 33.55 6.14 135.99 465000.00 186.80 537.85 747.96 25.56 5206.93 11.85 1.14 BDDL 0.42 0.65 0.44 6.57 0.06 0.19 0.59 0.43 3.60 4.49 0.01 0.44Precision(%) 13.02 16.72 8.48 3.52 3.82 4.24 17.12 5.70 5.90 15.56 17.73

Golden Mile Fimiston Depth D12-1A Conc. (ppm) 6.59 BD 13.39 465000.00 10.48 183.44 70.84 41.13 4712.45 BD 0.04 BDDL 0.30 0.81 0.53 6.21 0.04 0.14 0.75 0.29 3.49 6.26 0.02 0.45Precision(%) 9.40 12.95 3.60 4.25 5.84 10.77 4.76 5.75 47.31

Golden Mile Fimiston Depth D12-2 Conc. (ppm) 1102.35 1.02 194.69 465000.00 367.87 591.05 347.29 26.64 3784.86 8.36 19.56 BDDL 0.46 0.79 0.53 7.76 0.06 0.16 0.69 0.35 4.25 5.34 0.02 0.50Precision(%) 12.52 34.26 10.44 3.40 3.54 5.34 6.17 4.97 4.05 25.91 9.84

Golden Mile Fimiston Depth D14_1 Conc. (ppm) 6.56 BD BD 465000.00 16.52 60.72 253.26 1.38 1270.04 23.85 BD BDDL 0.46 0.96 0.55 8.05 0.04 0.23 0.73 0.33 4.46 5.63 0.01 0.49Precision(%) 6.65 3.43 10.25 10.88 9.23 27.50 4.42 11.67

Golden Mile Fimiston Depth D14_2C Conc. (ppm) 5.53 BD BD 465000.00 13.92 157.72 387.41 1.55 223.36 115.92 BD BDDL 0.62 0.73 0.58 7.45 0.05 0.21 0.71 0.28 4.28 4.54 0.02 0.51Precision(%) 8.61 3.64 3.52 3.95 8.78 12.82 3.96 4.67

Golden Mile Fimiston Depth D14_2R Conc. (ppm) 7.89 BD 123.90 465000.00 4.31 175.45 560.43 15.38 4755.80 54.27 BD BDDL 0.44 0.81 0.55 9.09 0.04 0.17 0.77 0.34 4.47 4.65 0.03 0.55Precision(%) 6.18 17.12 3.52 8.49 4.67 5.37 15.24 4.55 6.60

Golden Mile Fimiston Depth D14_3C Conc. (ppm) 9.41 BD BD 465000.00 9.69 251.63 381.12 2.12 1198.01 24.65 BD BDDL 0.45 0.76 0.50 9.79 0.07 0.16 0.62 0.41 3.75 3.95 0.02 0.48

344




D1_1-1 Conc. (ppm)DLPrecision(%)





d12_4 Conc. (ppm)DLPrecision(%)

d12_5 Conc. (ppm)DLPrecision(%)

d12_5-2 Conc. (ppm)DLPrecision(%)

D12-1 Conc. (ppm)DLPrecision(%)

D12-1A Conc. (ppm)DLPrecision(%)

D12-2 Conc. (ppm)DLPrecision(%)

D14_1 Conc. (ppm)DLPrecision(%)

D14_2C Conc. (ppm)DLPrecision(%)

D14_2R Conc. (ppm)DLPrecision(%)

D14_3C Conc. (ppm)DL


17.28 13.32 13.04 12.04 21.47 14.81 17.14 13.55 13.20 32.84 29.88 43.541.45 1.94 0.60 10.43 BD 13.17 0.01 1.91 33.21 0.11 9.73 BD 0.08 0.010.09 2.59 0.09 0.09 0.94 0.07 0.01 0.02 0.03 0.01 0.02 0.01 0.01 0.01

33.92 50.27 8.17 5.91 14.90 31.01 7.24 32.62 12.01 7.37 8.76 28.221.42 BD 0.67 34.23 BD 6.59 0.38 68.74 43.03 BD 37.21 0.04 0.32 0.050.08 2.66 0.11 0.04 1.20 0.06 0.01 0.03 0.04 0.02 0.02 0.01 0.01 0.00

17.12 11.26 9.86 23.40 30.97 35.28 17.94 5.75 15.57 28.08 22.02105.81 BD 0.82 16.91 171.22 1.96 0.04 1.78 200.06 0.15 35.82 0.10 BD BD

0.09 2.63 0.11 0.06 1.33 0.09 0.01 0.00 0.03 0.01 0.02 0.02 0.01 0.0119.47 8.59 9.96 13.47 15.54 19.95 14.84 55.05 7.93 4.89 12.17

0.11 BD 1.06 2.14 BD BD BD BD 0.71 BD 5.67 BD BD BD0.10 2.48 0.16 0.08 1.47 0.10 0.01 0.03 0.04 0.02 0.03 0.01 0.01 0.01

47.31 7.33 8.56 10.71 8.313.01 BD 0.99 19.28 24.13 6.51 0.02 0.76 7.70 0.18 28.34 0.02 BD BD0.09 2.99 0.14 0.07 1.41 0.07 0.01 0.03 0.03 0.02 0.03 0.01 0.01 0.017.00 7.17 4.26 8.78 18.98 57.06 20.05 7.11 9.48 3.44 24.303.70 BD 1.01 16.12 29.94 4.32 0.05 3.11 8.87 0.27 45.28 0.04 0.04 BD0.12 3.20 0.16 0.08 1.69 0.14 0.01 0.04 0.05 0.01 0.04 0.01 0.01 0.017.33 7.88 5.76 7.30 13.36 18.30 13.06 7.44 8.55 5.94 17.57 24.131.53 BD 0.83 15.87 9.93 1.14 0.17 1.16 0.86 0.75 73.51 0.03 BD BD0.08 2.55 0.14 0.05 1.29 0.08 0.01 0.03 0.04 0.01 0.03 0.00 0.01 0.019.27 9.05 4.72 11.31 8.64 12.78 14.15 11.52 5.51 4.54 17.273.91 BD 3.01 19.14 3.28 0.24 0.02 2.50 0.91 0.02 26.28 3.57 BD BD0.10 2.36 0.16 0.09 1.30 0.08 0.01 0.04 0.04 0.01 0.03 0.01 0.01 0.014.54 4.51 3.09 19.98 26.55 33.64 45.99 7.78 34.38 2.80 3.14

BD BD 31.34 BD BD BD 0.91 3.98 BD BD 35.17 1.27 BD BD5.84 199.76 11.28 6.48 93.53 5.35 0.57 1.59 1.59 1.23 1.66 0.81 0.40 0.47

17.46 36.46 28.36 16.53 31.902.80 BD 2.82 11.35 BD 0.13 0.14 1.22 0.47 0.04 15.48 1.50 4.85 BD0.12 4.07 0.25 0.11 2.11 0.11 0.02 0.08 0.05 0.02 0.05 0.02 0.01 0.02

46.02 16.69 11.31 41.82 25.71 12.34 16.55 33.07 10.10 13.29 100.612.40 BD 2.05 18.66 3.57 BD 0.73 0.77 0.66 0.06 31.97 2.33 0.01 BD0.10 2.34 0.14 0.05 1.23 0.12 0.01 0.04 0.04 0.01 0.03 0.01 0.00 0.015.98 5.44 7.52 18.18 27.20 22.80 8.15 14.06 7.33 4.02 30.800.63 BD 2.22 4.17 1.57 BD BD 0.07 0.42 0.02 3.61 0.59 BD BD0.09 2.59 0.13 0.05 1.11 0.08 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.01

10.96 5.48 5.79 32.19 32.88 11.60 32.75 5.26 6.602.07 BD 4.60 17.91 BD 0.64 0.07 41.65 0.79 0.10 19.90 2.24 BD BD0.12 2.11 0.15 0.06 1.12 0.09 0.01 0.05 0.05 0.02 0.03 0.01 0.01 0.016.12 5.80 3.62 14.64 31.95 21.21 7.92 13.52 3.89 4.173.09 2.47 1.36 1.59 131.02 0.04 BD BD 4.97 0.04 3.31 0.35 BD BD0.10 2.20 0.16 0.04 1.43 0.11 0.01 0.03 0.03 0.01 0.03 0.02 0.01 0.008.62 36.18 7.12 13.70 9.39 132.30 10.90 20.58 8.47 18.21

18.64 BD 1.22 2.25 296.27 BD BD BD 35.60 BD 5.05 0.53 BD BD0.10 3.01 0.17 0.05 1.25 0.10 0.01 0.02 0.06 0.01 0.02 0.01 0.01 0.005.23 7.51 6.40 5.49 6.90 3.85 6.60

45.03 BD 0.97 7.44 2157.98 BD 0.06 BD 507.60 0.05 16.97 1.66 BD BD0.12 2.61 0.14 0.07 1.40 0.12 0.01 0.04 0.05 0.01 0.03 0.01 0.01 0.016.10 7.84 4.81 6.25 20.74 7.22 16.03 4.28 8.312.17 BD 1.08 2.03 154.59 1.23 BD BD 7.01 0.17 6.32 0.95 BD BD0.11 2.41 0.18 0.06 1.45 0.08 0.01 0.04 0.04 0.01 0.03 0.01 0.01 0.00

345

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Precision(%) 6.49 3.67 10.61 9.97 7.22 15.67 4.72 8.54

Golden Mile Fimiston Depth D14_3R Conc. (ppm) 7.59 BD BD 465000.00 30.84 336.00 36.34 0.89 333.05 15.69 BD BDDL 0.58 0.80 0.46 11.20 0.05 0.15 0.76 0.45 3.86 4.12 0.02 0.49Precision(%) 8.06 3.60 4.06 3.41 11.64 24.96 4.69 12.21

Golden Mile Fimiston Depth D4_2 Conc. (ppm) 300.75 BD 1.09 465000.00 209.97 54.02 33.03 0.65 378.89 4.21 1.47 0.53DL 0.66 0.70 0.50 12.42 0.08 0.16 0.63 0.49 5.22 3.94 0.01 0.51Precision(%) 16.21 22.86 3.30 6.22 4.41 24.18 35.40 23.30 38.88 21.92 39.25

Golden Mile Fimiston Depth D4_3 Conc. (ppm) 943.21 BD 25.93 465000.00 664.36 53.29 130.10 15.57 1821.20 8.47 7.27 BDDL 0.54 0.71 0.65 10.85 0.05 0.21 0.68 0.33 5.34 4.76 0.02 0.66Precision(%) 13.21 8.12 2.53 10.76 7.07 8.46 10.75 11.75 23.37 14.62

Golden Mile Fimiston Depth D4_4 Conc. (ppm) 551.13 BD 80.61 465000.00 671.55 16.62 168.15 10.48 3966.26 7.96 21.49 BDDL 0.66 0.98 0.79 17.30 0.08 0.29 0.91 0.38 6.15 6.06 0.02 0.73Precision(%) 17.98 14.48 8.41 9.32 9.34 22.66 13.51 8.83 34.48 23.56

Golden Mile Eastern Lode Great Boulder Main GBM_3-1 Conc. (ppm) 9.27 BD 23.38 465000.00 67.96 25.58 0.59 2.72 BD BD 0.32 BDDL 0.40 0.76 0.38 10.94 0.04 0.15 0.52 0.29 2.43 3.61 0.01 0.52Precision(%) 6.44 16.54 2.87 3.44 3.18 40.03 12.30 27.47

Golden Mile Eastern Lode Great Boulder Main GBM_3-2 Conc. (ppm) 17.99 BD 265.78 465000.00 71.28 20.46 1.87 10.60 22.99 BD 32.22 BDDL 0.52 0.71 0.53 23.82 0.07 0.12 0.46 0.39 2.14 3.80 0.01 0.59Precision(%) 13.62 17.07 3.61 5.99 5.23 18.03 15.32 13.68 28.59

Golden Mile Eastern Lode Great Boulder Main GBM59_1-1 Conc. (ppm) 6.67 BD BD 465000.00 107.42 12.03 BD 1.08 490.45 13.46 3.23 BDDL 0.45 0.66 0.40 15.07 0.04 0.13 0.57 0.22 2.05 3.86 0.01 0.39Precision(%) 6.54 3.52 7.38 5.48 14.50 4.54 13.21 42.28

Golden Mile Eastern Lode Great Boulder Main GBM59_1-2 Conc. (ppm) 22.83 BD 27.57 465000.00 224.25 22.56 6.76 54.12 163.08 10.63 0.21 BDDL 0.30 0.53 0.33 16.49 0.03 0.15 0.33 0.24 1.80 3.06 0.02 0.39Precision(%) 17.33 10.90 2.94 6.80 10.08 15.57 12.37 10.17 13.01 17.93

Golden Mile Eastern Lode Great Boulder Main GBM59_2-1 Conc. (ppm) 6.51 BD BD 465000.00 1459.17 9.31 0.39 1.36 1063.59 15.53 BD BDDL 0.58 0.56 0.50 18.08 0.05 0.11 0.62 0.30 8.28 3.86 0.02 0.51Precision(%) 7.15 3.99 7.11 5.15 62.77 13.76 6.07 11.90


Golden Mile Eastern Lode Great Boulder Main GBM59_4 Conc. (ppm) 7.07 BD 7.25 465000.00 102.98 12.38 BD 1.61 36.39 4.79 BD BDDL 0.55 0.54 0.47 28.21 0.05 0.11 0.44 0.32 2.41 3.50 0.02 0.47Precision(%) 6.48 55.42 3.84 7.42 6.69 17.73 6.90 31.32

Golden Mile Eastern Lode Great Boulder Main GBM76_1 Conc. (ppm) 14.59 BD 1.81 465000.00 132.49 16.13 63.28 1.22 189.30 7.49 BD BDDL 0.48 0.65 0.42 6.79 0.05 0.17 0.49 0.19 1.88 5.52 0.02 0.47Precision(%) 20.43 42.16 3.25 16.00 6.64 45.32 11.87 7.72 29.11

Golden Mile Eastern Lode Great Boulder Main GBM76_2 Conc. (ppm) 8.08 BD 105.39 465000.00 68.14 39.62 6.17 4.80 148.37 3.89 BD BDDL 0.53 0.90 0.50 9.94 0.05 0.16 0.53 0.40 1.88 4.75 0.02 0.50Precision(%) 6.62 18.11 3.21 5.73 4.63 14.41 32.00 4.78 45.29

Golden Mile Eastern Lode Great Boulder Main GBM76_3-1 Conc. (ppm) 8.99 BD 1.43 465000.00 49.33 5.86 12.39 3.52 452.99 6.82 BD BDDL 0.48 0.66 0.44 15.27 0.04 0.15 0.56 0.41 2.37 5.24 0.02 0.55Precision(%) 25.13 15.16 3.10 11.95 14.25 20.06 29.30 8.15 35.45

Golden Mile Eastern Lode Great Boulder Main GBM76_3-2 Conc. (ppm) 20.73 3.05 14197.97 465000.00 60.18 22.47 10.66 305.71 534.41 BD 0.15 BDDL 2.21 2.66 1.78 154.36 0.19 0.98 1.80 1.43 9.69 16.65 0.06 2.30Precision(%) 17.82 36.04 9.53 13.02 19.15 13.35 19.90 9.61 14.59 29.59

Golden Mile Eastern Lode Great Boulder Main GBM78_1-1 Conc. (ppm) 15.37 0.97 0.55 465000.00 481.77 305.34 1161.37 62.09 5490.42 20.10 BD BDDL 0.40 0.59 0.47 8.68 0.04 0.12 0.42 0.23 4.07 4.43 0.02 0.45Precision(%) 10.22 30.30 32.51 3.51 5.45 3.54 14.20 12.91 12.69 10.01

Golden Mile Eastern Lode Great Boulder Main GBM78_1-2 Conc. (ppm) 687.80 16.94 1.83 465000.00 484.97 356.29 194.97 6.43 5785.48 17.37 83.45 BDDL 0.51 1.08 0.69 12.61 0.06 0.31 0.60 0.36 6.26 6.36 0.04 0.95Precision(%) 16.44 13.21 19.85 13.39 13.00 13.42 20.85 13.00 17.63 18.87 15.00

346


D14_3R Conc. (ppm)DLPrecision(%)




GBM_3-1 Conc. (ppm)DLPrecision(%)

GBM_3-2 Conc. (ppm)DLPrecision(%)

GBM59_1-1 Conc. (ppm)DLPrecision(%)




GBM59_4 Conc. (ppm)DLPrecision(%)







Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2387.97 8.16 6.95 6.09 17.18 10.34 9.97 7.49 5.821.91 BD 1.06 2.36 23.44 BD BD 0.06 3.48 BD 1.26 0.08 BD BD0.11 2.87 0.14 0.07 1.27 0.07 0.01 0.02 0.07 0.02 0.02 0.01 0.01 0.01

10.61 7.20 19.05 9.93 32.23 10.00 10.73 12.1347.26 BD 1.71 3.67 87.04 0.35 0.02 3.23 22.86 0.07 7.27 BD BD BD0.10 2.98 0.16 0.06 1.08 0.09 0.01 0.05 0.03 0.02 0.03 0.02 0.00 0.01

22.06 5.64 17.26 15.35 22.37 35.78 39.10 22.33 20.45 12.2320.58 BD 2.42 45.48 116.17 9.01 0.04 3.10 18.82 1.75 80.65 0.20 0.03 BD0.11 2.29 0.15 0.07 1.43 0.08 0.01 0.04 0.04 0.01 0.03 0.01 0.00 0.01

10.89 5.35 11.77 11.27 11.03 18.50 10.09 10.39 12.06 10.80 11.45 19.8517.84 BD 1.28 15.21 65.51 72.68 0.06 8.63 34.11 0.58 25.45 0.11 0.06 0.020.13 3.39 0.18 0.07 1.40 0.12 0.01 0.03 0.06 0.02 0.04 0.02 0.01 0.01

10.34 10.02 11.44 9.33 9.95 16.41 15.55 9.69 11.03 9.23 14.67 22.10 26.33BD BD 0.79 BD 2.26 BD BD 0.12 0.19 BD 0.58 BD BD BD

0.08 2.26 0.14 0.06 1.24 0.05 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.018.17 33.61 22.83 26.23 17.29

BD BD 0.86 0.69 8.28 0.11 0.03 0.32 0.13 BD 3.39 BD BD 0.020.08 2.50 0.15 0.05 1.09 0.10 0.01 0.03 0.04 0.02 0.03 0.02 0.01 0.01

8.62 14.32 11.87 46.86 41.44 16.97 18.79 10.80 41.53BD BD 0.82 BD 1.02 BD 0.02 BD BD BD 0.08 BD BD BD

0.08 2.19 0.13 0.09 0.83 0.06 0.01 0.04 0.03 0.01 0.02 0.01 0.01 0.018.02 36.83 78.39 30.42

0.70 BD 8.16 1.71 16.17 1.42 0.02 0.13 0.90 0.03 36.46 0.07 BD BD0.06 1.90 0.11 0.08 0.83 0.07 0.01 0.03 0.04 0.01 0.02 0.01 0.01 0.01

12.88 16.93 11.75 11.01 13.07 24.11 21.88 12.21 21.21 15.45 19.57BD BD 0.69 0.07 1.35 BD BD BD 0.08 BD 0.05 BD BD BD

0.07 2.32 0.12 0.06 1.15 0.07 0.00 0.03 0.03 0.02 0.03 0.01 0.01 0.008.82 43.09 41.28 32.02 36.16

0.15 BD 0.62 0.19 4.26 BD BD BD 0.08 BD 1.46 0.02 BD BD0.09 2.39 0.12 0.09 1.15 0.10 0.01 0.04 0.04 0.01 0.02 0.01 0.01 0.01

33.65 9.93 29.97 20.24 38.92 26.01 29.720.14 BD 0.69 0.08 3.62 BD BD BD 0.07 BD 0.38 BD BD BD0.08 2.66 0.13 0.06 1.33 0.05 0.01 0.03 0.05 0.02 0.03 0.01 0.01 0.01

29.73 9.74 38.11 19.16 38.73 19.110.43 BD 0.84 0.21 9.27 0.04 BD 0.21 0.08 BD 0.94 BD BD BD0.06 2.65 0.14 0.06 1.25 0.05 0.01 0.04 0.04 0.01 0.03 0.01 0.00 0.01

26.43 9.19 22.97 10.91 72.45 33.01 30.31 26.740.09 BD 0.86 2.99 7.37 0.26 0.08 0.06 0.10 BD 1.66 BD BD BD0.05 2.14 0.14 0.07 0.92 0.05 0.01 0.03 0.04 0.02 0.02 0.01 0.01 0.01

30.77 7.91 7.99 10.72 30.18 46.91 38.97 23.33 7.20BD BD 0.64 2.93 2.83 BD BD BD 0.28 BD 2.47 BD BD BD

0.10 3.19 0.15 0.07 1.33 0.07 0.01 0.05 0.04 0.03 0.03 0.01 0.01 0.0114.27 17.19 31.17 27.70 16.57

BD BD 4.18 1.73 BD 3.68 1.34 0.29 0.38 BD 3.25 BD BD BD0.32 12.06 0.54 0.27 5.87 0.25 0.05 0.26 0.07 0.09 0.09 0.06 0.03 0.01

11.35 19.09 12.45 10.72 40.53 23.72 15.3010.80 BD 0.56 33.68 20.86 3.02 BD 0.12 32.68 2.57 21.23 BD BD BD0.08 3.37 0.11 0.06 1.23 0.05 0.01 0.03 0.05 0.01 0.02 0.01 0.01 0.01

22.57 10.61 11.67 14.27 16.12 20.93 18.04 10.65 12.6627.33 BD 2.04 28.22 84.84 95.42 BD 6.42 24.31 2.16 9.41 0.17 0.10 0.070.16 4.45 0.20 0.12 2.60 0.15 0.01 0.11 0.08 0.02 0.03 0.02 0.01 0.01

16.92 12.30 14.36 13.81 12.08 22.81 19.48 11.30 13.90 14.68 19.29 20.25

347

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Golden Mile Eastern Lode Great Boulder Main GBM78_2-1 Conc. (ppm) 1604.73 44.08 4.51 465000.00 699.92 376.87 150.23 18.95 3787.28 19.52 5.44 BD

DL 0.47 0.83 0.55 14.07 0.10 0.16 0.73 0.39 4.44 6.75 0.03 0.84Precision(%) 12.03 13.60 57.30 10.26 13.65 11.53 19.36 35.39 14.38 18.30 14.80


Golden Mile Eastern Lode Great Boulder Main GBM78_3-1 Conc. (ppm) 6.55 BD 0.90 465000.00 10.88 549.72 1.13 0.79 89.98 21.50 BD BDDL 0.48 0.60 0.43 6.18 0.03 0.10 0.38 0.24 3.53 4.45 0.01 0.50Precision(%) 7.73 26.37 3.93 12.76 9.61 18.67 18.83 5.77 9.35

Golden Mile Eastern Lode Great Boulder Main GBM78_3-2 Conc. (ppm) 7.05 BD 0.78 465000.00 118.89 324.88 BD 0.86 422.74 27.78 BD BDDL 0.45 0.72 0.45 5.54 0.06 0.19 0.48 0.39 3.69 5.11 0.02 0.58Precision(%) 6.66 22.23 3.77 4.52 4.71 21.07 5.90 8.68








Golden Mile Eastern Lode Great Boulder Main GBM97_1-2 Conc. (ppm) 24.85 6.25 21.69 465000.00 41.87 98.43 591.58 14.52 9982.95 37.80 0.07 6.80DL 0.44 0.51 0.42 6.36 0.08 0.15 0.44 0.25 2.40 3.82 0.02 0.49Precision(%) 17.57 13.09 11.65 2.98 7.04 5.38 13.65 10.16 6.60 9.42 25.11 12.60


Golden Mile Eastern Lode Great Boulder Main GBM97_2-2 Conc. (ppm) 50.65 BD 70.53 465000.00 203.02 178.24 300.29 15.69 12106.71 106.99 0.41 0.73DL 0.51 0.78 0.46 18.30 0.05 0.17 0.44 0.24 2.96 4.62 0.01 0.50Precision(%) 15.24 10.78 3.10 6.94 5.00 15.15 12.25 10.02 7.47 25.89 34.35

Golden Mile Eastern Lode Great Boulder Main GBM97_3 Conc. (ppm) 137.13 BD 14.33 465000.00 228.29 92.66 205.42 10.52 1947.19 93.08 3.34 0.85DL 0.43 0.56 0.39 13.56 0.04 0.17 0.41 0.24 3.18 4.73 0.02 0.54Precision(%) 13.90 8.27 3.59 5.45 7.48 18.47 9.81 11.07 5.15 25.87 27.23

Golden Mile Western Lode Lake View LV27_2 Conc. (ppm) 127.10 BD 2.79 465000.00 275.20 161.26 108.50 8.30 627.95 20.03 4.30 BDDL 0.43 0.88 0.63 10.49 0.05 0.17 0.85 0.38 4.73 5.65 0.02 0.73Precision(%) 19.23 11.08 5.43 5.82 4.55 17.06 10.23 8.42 12.27 13.12

Golden Mile Western Lode Lake View LV27-1 Conc. (ppm) 509.11 0.77 17.65 465000.00 203.78 179.40 185.59 64.16 269.78 14.65 0.46 BDDL 0.83 0.64 0.62 10.36 0.06 0.20 1.00 0.49 5.39 4.82 0.03 0.73Precision(%) 34.65 39.23 17.00 8.35 8.57 8.23 8.89 17.42 8.75 15.41 25.57

Golden Mile Western Lode Lake View LV27-3 Conc. (ppm) 101.11 BD 1.28 465000.00 1077.21 461.94 26.80 6.13 287.90 26.42 9.26 BD

348

Sample NoGBM78_2-1 Conc. (ppm)

DLPrecision(%)















LV27_2 Conc. (ppm)DLPrecision(%)

LV27-1 Conc. (ppm)DLPrecision(%)

LV27-3 Conc. (ppm)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23812.91 BD 1.22 21.83 65.50 84.33 0.03 9.50 22.24 1.54 9.12 0.03 BD BD0.15 4.56 0.21 0.08 1.60 0.09 0.01 0.04 0.05 0.02 0.03 0.02 0.01 0.01

11.03 10.89 11.33 11.65 15.20 24.94 11.73 15.60 12.91 11.35 28.4127.24 BD 1.20 18.96 69.80 48.81 BD 0.91 26.95 0.81 3.17 0.08 BD BD0.09 3.69 0.12 0.08 1.98 0.08 0.01 0.04 0.05 0.02 0.02 0.01 0.01 0.01

10.17 9.13 12.09 9.58 12.56 12.11 8.37 9.19 8.05 15.768.42 BD 0.47 0.22 14.25 BD BD BD 2.67 BD 1.14 0.06 BD BD0.11 2.84 0.13 0.08 1.63 0.07 0.01 0.04 0.03 0.02 0.02 0.01 0.01 0.01

34.53 13.04 21.19 14.16 18.11 7.58 17.58BD BD 0.44 BD BD BD BD BD BD BD BD BD BD BD

0.11 2.88 0.13 0.06 1.35 0.04 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.0113.05

5.00 BD 2.17 8.36 49.57 86.46 1.75 8.46 13.99 0.68 3.06 BD 0.03 BD0.18 5.72 0.24 0.12 2.70 0.14 0.02 0.06 0.12 0.03 0.05 0.02 0.02 0.02

20.59 12.06 17.50 19.83 13.92 14.57 20.61 20.74 13.27 13.17 28.636.98 BD 2.76 45.72 62.90 116.77 0.22 2.99 14.22 1.30 6.97 BD BD BD0.27 7.35 0.24 0.11 3.01 0.22 0.02 0.04 0.16 0.04 0.08 0.03 0.02 0.02

20.33 14.91 22.54 20.32 14.65 15.76 19.11 22.52 16.55 17.877.89 BD 1.55 11.96 84.32 30.65 0.19 0.15 14.52 1.62 4.92 BD BD BD0.19 5.97 0.22 0.14 1.99 0.10 0.03 0.09 0.14 0.03 0.05 0.03 0.01 0.01

19.66 13.99 18.06 18.78 16.84 17.39 33.05 19.41 17.11 17.359.80 BD 2.45 21.08 82.41 75.23 0.46 1.16 16.60 1.32 5.34 0.04 BD BD0.13 4.24 0.22 0.13 2.03 0.15 0.01 0.08 0.08 0.02 0.05 0.02 0.02 0.01

20.11 12.33 25.31 18.66 13.11 15.48 19.33 19.26 13.92 16.73 32.0512.52 BD 0.47 8.92 71.78 4.18 0.03 3.89 36.97 0.32 2.22 BD 0.07 0.030.08 2.36 0.12 0.05 1.31 0.06 0.00 0.04 0.05 0.01 0.03 0.02 0.01 0.019.44 13.39 10.44 7.94 30.75 16.11 9.96 13.02 10.64 8.35 29.66 22.31

80.94 BD 0.60 3.98 105.85 21.66 0.03 2.32 38.70 0.27 3.12 0.02 0.02 BD0.10 2.26 0.13 0.06 1.53 0.08 0.01 0.04 0.04 0.02 0.02 0.01 0.01 0.01

26.54 12.31 13.74 18.60 15.61 19.34 12.39 17.62 9.07 5.94 33.38 30.217.19 BD 0.81 29.59 BD 3.91 0.02 0.06 3.16 0.08 41.73 0.22 BD BD0.08 2.53 0.13 0.06 1.29 0.07 0.01 0.04 0.05 0.01 0.03 0.01 0.01 0.016.59 8.67 17.29 10.76 34.26 33.78 6.20 9.31 4.51 6.959.70 BD 0.70 71.96 1.54 0.12 BD BD 2.48 0.20 122.41 0.44 BD BD0.10 2.62 0.10 0.04 1.03 0.08 0.01 0.05 0.04 0.01 0.02 0.02 0.01 0.01

13.05 8.46 15.34 33.07 35.39 10.20 11.75 9.70 8.523.87 BD 0.83 52.42 2.71 0.23 BD BD 1.94 0.14 211.90 0.64 BD BD0.07 2.82 0.12 0.07 1.72 0.08 0.01 0.04 0.04 0.02 0.02 0.01 0.01 0.016.45 7.66 4.68 27.42 20.28 19.41 9.05 4.24 6.123.89 BD 0.85 45.22 2.27 5.54 0.02 0.04 2.12 0.09 83.41 0.43 BD BD0.08 2.46 0.11 0.05 1.06 0.09 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.01

11.83 7.43 11.77 23.67 30.61 23.92 37.25 13.52 15.69 7.19 11.033.81 BD 0.85 69.13 1.60 0.74 BD 0.06 0.69 0.18 233.31 1.98 0.01 BD0.10 2.50 0.14 0.07 1.54 0.09 0.01 0.04 0.06 0.01 0.02 0.01 0.01 0.01

12.27 8.26 12.53 39.37 11.94 33.37 12.35 10.72 9.69 7.37 43.690.41 BD 0.84 3.14 BD 22.98 BD 0.34 0.95 0.15 5.67 0.60 BD BD0.11 3.60 0.20 0.07 1.98 0.10 0.01 0.03 0.06 0.02 0.02 0.02 0.01 0.01

15.38 11.33 7.34 13.16 22.12 10.10 10.47 5.04 5.851.77 BD 0.99 9.85 BD 48.67 BD 0.66 3.80 0.27 20.89 2.50 BD BD0.11 3.14 0.18 0.09 1.58 0.13 0.01 0.04 0.04 0.02 0.03 0.01 0.01 0.01

11.69 10.45 8.70 15.64 24.48 12.35 11.86 8.67 9.07BD BD 1.11 0.85 BD 11.46 BD 0.34 0.14 0.07 0.92 0.12 0.11 0.01

349

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95DL 0.76 0.79 0.57 8.89 0.07 0.21 0.88 0.24 5.02 4.25 0.02 0.68Precision(%) 14.78 20.08 6.97 8.02 6.42 14.51 14.87 7.75 9.85 18.87


Golden Mile Western Lode Lake View LV29_2-1A Conc. (ppm) 53884.65 2.01 10.36 465000.00 488.95 83.18 566.41 15.71 1813.28 7.19 123.22 BDDL 0.61 0.52 0.64 10.18 0.06 0.27 0.89 0.44 4.39 6.68 0.03 0.77Precision(%) 8.82 15.65 9.06 4.82 5.76 5.87 9.07 8.93 6.06 37.04 20.35

Golden Mile Western Lode Lake View LV29_2-1B Conc. (ppm) 3569.95 BD 241.99 465000.00 259.13 37.32 353.74 119.32 5414.86 BD 4.01 BDDL 1.17 1.21 1.00 14.77 0.09 0.40 1.07 0.67 6.45 8.74 0.04 0.85Precision(%) 16.38 15.06 13.85 12.90 14.57 16.95 13.88 14.91 26.67


Golden Mile Western Lode Lake View LV37_1-1 Conc. (ppm) 162.50 BD 63.99 465000.00 199.38 115.09 281.65 14.40 8985.63 BD 5.95 BDDL 0.46 0.68 0.51 10.00 0.06 0.16 0.53 0.17 3.82 5.24 0.03 0.53Precision(%) 6.94 4.84 3.35 3.84 3.59 13.06 5.16 3.94 16.08

Golden Mile Western Lode Lake View LV37_1-2 Conc. (ppm) 13.62 BD 3542.38 465000.00 685.18 233.78 16.63 81.94 470.19 21.47 1.81 0.75DL 0.78 0.91 0.75 12.95 0.07 0.38 0.94 0.43 5.17 6.63 0.03 0.72Precision(%) 13.97 11.03 9.41 10.77 11.75 14.27 10.71 13.51 17.91 26.67 37.82

Golden Mile Western Lode Lake View LV37_2-1 Conc. (ppm) 497.88 BD 180.42 465000.00 53.92 106.84 139.76 5.43 2747.85 10.80 17.75 BDDL 0.54 0.85 0.59 9.22 0.06 0.15 0.71 0.56 3.46 5.68 0.02 0.70Precision(%) 7.95 14.38 3.58 5.17 6.37 18.92 12.31 7.61 21.83 11.55




Golden Mile Western Lode Lake View LV46_1 Conc. (ppm) 37.44 BD 277.07 465000.00 564.58 61.18 208.54 15.50 580.17 22.86 3.27 0.67DL 0.48 0.97 0.61 7.05 0.04 0.12 0.77 0.34 2.87 4.50 0.02 0.58Precision(%) 23.02 10.45 2.81 12.91 4.64 19.97 25.15 5.26 12.02 57.99 37.52




Golden Mile Western Lode Lake View LV47_1-1 Conc. (ppm) 6.98 BD 1.41 465000.00 162.34 9.56 70.61 1.14 5678.70 17.01 BD BDDL 0.34 0.53 0.41 7.74 0.04 0.14 0.59 0.18 2.88 3.47 0.02 0.53Precision(%) 6.84 14.05 3.35 14.74 58.99 11.28 13.95 4.41 10.48

Golden Mile Western Lode Lake View LV47_1-2 Conc. (ppm) 6.73 BD BD 465000.00 3.09 10.46 3.85 1.41 18.30 29.78 0.03 BDDL 0.75 1.12 0.62 29.44 0.07 0.26 0.83 0.42 4.15 5.01 0.02 0.88Precision(%) 8.15 2.40 10.70 4.18 11.32 18.41 9.82 8.86 41.65

Golden Mile Western Lode Lake View LV47_2-1 Conc. (ppm) 6.32 BD 0.70 465000.00 3.47 3.52 BD 0.97 8.02 20.83 BD BDDL 0.40 0.68 0.42 8.07 0.05 0.19 0.72 0.43 3.22 4.57 0.02 0.47

350



LV29_2-1A Conc. (ppm)DLPrecision(%)

LV29_2-1B Conc. (ppm)DLPrecision(%)


LV37_1-1 Conc. (ppm)DLPrecision(%)












LV47_2-1 Conc. (ppm)DL


10.03 11.79 17.01 17.26 23.04 14.52 10.64 14.02 19.71 46.470.16 BD 0.73 2.94 2.23 7.22 BD 0.02 17.78 0.10 0.53 BD BD BD0.11 2.21 0.16 0.08 1.54 0.10 0.01 0.00 0.06 0.02 0.02 0.01 0.01 0.01

30.69 11.39 5.83 30.99 40.94 35.83 7.60 13.46 12.313.13 BD 6.76 69.19 30.78 12.66 3.54 948.70 10.64 1.35 20.69 0.63 0.54 0.300.14 3.65 0.19 0.09 1.59 0.20 0.01 0.06 0.04 0.02 0.03 0.01 0.01 0.018.45 7.76 6.27 7.86 6.62 5.95 5.62 7.41 5.10 6.24 8.50 12.06 12.800.83 BD 2.34 15.72 14.07 29.08 0.25 79.66 18.13 0.65 4.80 0.15 0.03 BD0.16 4.61 0.27 0.12 2.25 0.14 0.02 0.08 0.10 0.03 0.05 0.02 0.01 0.01

16.33 12.14 13.58 14.97 13.95 19.32 18.12 15.48 13.41 12.14 15.79 26.950.51 BD 0.91 3.36 10.05 0.73 0.11 8.57 0.98 0.21 4.30 0.11 0.17 0.020.11 3.09 0.17 0.08 1.65 0.10 0.01 0.05 0.02 0.01 0.03 0.02 0.01 0.01

13.19 10.03 6.19 11.37 12.24 12.66 16.20 9.21 8.80 4.37 11.71 18.56 25.182.51 BD 1.00 86.90 5.53 0.33 0.02 6.92 83.46 4.06 1.30 BD 0.02 BD0.06 2.82 0.14 0.07 1.28 0.08 0.01 0.05 0.03 0.01 0.03 0.02 0.00 0.015.95 7.71 3.61 21.85 18.66 23.55 7.18 5.71 4.16 7.86 17.770.44 BD 1.09 4.43 BD 1.56 0.15 0.18 3.60 0.23 8.38 BD BD BD0.13 3.50 0.24 0.13 1.77 0.15 0.01 0.07 0.05 0.02 0.03 0.02 0.01 0.01

20.65 11.96 20.26 14.78 12.79 29.59 16.96 26.14 14.491.09 BD 0.77 28.48 7.93 1.93 0.39 7.68 26.65 1.32 1.81 0.02 0.19 0.020.12 3.42 0.18 0.11 1.33 0.07 0.01 0.04 0.03 0.02 0.03 0.01 0.01 0.01

13.05 10.91 7.06 14.02 16.28 12.57 6.05 13.80 7.23 5.94 27.64 12.98 33.260.21 BD 1.07 0.43 BD 61.69 BD 1.59 1.12 0.24 0.56 BD BD BD0.12 3.40 0.21 0.08 2.41 0.16 0.01 0.03 0.07 0.02 0.03 0.02 0.01 0.01

34.73 10.64 19.93 15.32 24.44 21.79 14.33 13.560.80 BD 0.81 41.30 3.13 1.45 0.10 9.47 30.41 2.11 1.76 BD 0.04 0.020.11 3.03 0.14 0.10 1.12 0.06 0.01 0.06 0.04 0.02 0.03 0.01 0.01 0.01

10.26 9.07 6.88 19.07 18.99 14.47 8.18 6.72 8.48 5.92 16.94 27.241.24 BD 0.81 17.90 8.70 0.13 0.05 2.54 48.35 0.87 2.20 0.03 0.04 BD0.10 3.03 0.18 0.08 1.61 0.06 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.01

12.18 10.24 3.95 14.53 27.59 16.12 8.63 7.20 5.88 14.40 25.96 21.68191.70 BD 0.76 5.77 297.99 0.32 0.72 0.21 1950.82 0.40 12.54 0.07 BD BD

0.10 2.74 0.16 0.05 1.47 0.06 0.01 0.03 0.05 0.01 0.03 0.02 0.01 0.0125.43 10.02 9.83 11.31 18.36 29.75 28.86 31.43 13.21 6.11 26.62

1.43 BD 1.31 1.64 183.69 15.37 0.10 0.14 3.81 0.09 34.48 BD 0.15 0.030.14 3.95 0.21 0.11 1.78 0.11 0.02 0.05 0.02 0.03 0.04 0.02 0.01 0.01

12.39 11.18 10.35 7.62 18.65 17.43 22.70 10.60 18.12 12.90 20.74 22.0810.43 BD 0.87 1.44 135.05 1.24 0.24 0.11 16.37 0.05 3.32 BD 0.06 0.040.14 3.51 0.15 0.10 1.51 0.08 0.00 0.04 0.06 0.02 0.03 0.01 0.01 0.01

41.36 9.47 8.46 6.32 24.94 24.16 27.09 17.63 22.04 5.81 18.00 24.361.88 BD 0.65 21.17 33.18 0.20 2.56 1.92 1.48 0.65 22.03 BD 0.44 0.160.10 2.58 0.14 0.06 1.33 0.08 0.01 0.05 0.03 0.02 0.03 0.01 0.00 0.018.13 11.22 6.45 13.71 21.36 27.16 6.66 15.99 8.14 10.03 8.95 7.480.45 BD 0.73 6.89 4.05 0.32 BD 0.01 19.97 0.41 2.15 BD BD BD0.08 2.33 0.13 0.05 0.96 0.06 0.01 0.03 0.04 0.01 0.03 0.01 0.00 0.00

12.37 9.82 6.92 15.10 40.12 246.51 8.57 7.58 6.650.16 BD 1.11 0.71 BD 0.12 BD BD 0.27 BD 1.96 BD BD BD0.15 4.19 0.15 0.07 2.18 0.09 0.02 0.07 0.06 0.02 0.04 0.02 0.01 0.01

45.09 38.31 14.80 39.41 16.47 12.22BD BD 0.81 BD BD BD BD BD BD 0.02 BD BD BD BD

0.10 2.96 0.15 0.08 1.50 0.07 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.01

351

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Precision(%) 8.02 25.56 3.78 15.73 10.48 41.09 18.37 10.70

Golden Mile Western Lode Lake View LV47_2-2 Conc. (ppm) 97.70 BD BD 465000.00 19.84 3.63 44.23 0.64 4159.65 28.11 0.21 BDDL 0.49 0.74 0.45 10.05 0.05 0.19 0.65 0.46 3.23 5.32 0.02 0.47Precision(%) 14.97 3.35 3.73 7.99 17.71 31.20 7.65 8.87 22.56


Golden Mile Western Lode Lake View LV47_3 Conc. (ppm) 546.34 BD BD 465000.00 108.47 49.09 17.87 0.84 8908.41 28.42 7.15 BDDL 0.35 0.77 0.51 15.42 0.05 0.21 0.63 0.22 2.79 6.72 0.01 0.66Precision(%) 21.43 3.50 8.08 8.09 17.00 18.01 3.84 10.60 14.69

Golden Mile Western Lode Lake View LV53_1-2 Conc. (ppm) 75.89 4.09 71.34 465000.00 706.10 118.34 22.28 45.06 554.51 BD 0.37 BDDL 0.71 0.75 0.66 12.76 0.07 0.17 0.72 0.47 3.20 4.96 0.02 0.66Precision(%) 14.84 17.95 13.73 4.59 7.25 7.22 9.69 16.63 6.70 19.99



Golden Mile Western Lode Lake View LV53_4 Conc. (ppm) 775.66 40.76 279.83 465000.00 500.21 47.34 41.22 66.51 872.52 BD 17.31 BDDL 0.55 0.81 0.57 7.97 0.05 0.17 0.71 0.29 3.11 6.19 0.02 0.60Precision(%) 10.08 12.68 8.53 4.62 14.72 5.43 7.54 12.12 11.33 20.55



Golden Mile Western Lode Lake View LV56_1-1 Conc. (ppm) 950.52 BD 8.06 465000.00 262.84 156.71 121.48 25.17 4575.86 BD 9.61 1.12DL 0.70 1.30 1.05 12.98 0.11 0.28 0.97 0.58 5.34 10.95 0.02 0.73Precision(%) 15.46 17.67 14.96 14.93 14.94 18.29 26.10 15.72 16.40 30.22


Golden Mile Western Lode Lake View LV56_2-1 Conc. (ppm) 7.65 BD 117.97 465000.00 466.58 377.57 5.16 15.39 905.01 13.61 BD BDDL 0.73 0.68 0.58 7.74 0.06 0.19 0.68 0.31 2.85 5.60 0.02 0.58Precision(%) 7.37 33.20 3.55 8.92 6.10 17.13 35.22 5.25 17.67



Golden Mile Eastern Lode Oroya OR23_1 Conc. (ppm) 10.52 1.12 1.66 465000.00 128.91 138.54 18.18 BD BD 10.18 0.02 0.49DL 0.30 0.56 0.50 8.02 0.04 0.17 0.50 0.26 2.19 3.12 0.01 0.43Precision(%) 8.32 26.54 13.23 3.47 12.48 17.16 15.00 12.79 38.49 37.63

Golden Mile Eastern Lode Oroya OR23_2 Conc. (ppm) 14.89 BD 18.21 465000.00 230.98 91.43 77.84 3250.07 196.56 13.18 0.04 0.39DL 0.31 0.61 0.42 7.23 0.04 0.21 0.40 0.24 2.29 3.70 0.02 0.38Precision(%) 13.57 17.74 4.21 4.62 4.35 4.50 24.40 4.57 12.20 37.70 41.09

Golden Mile Eastern Lode Oroya OR23_3 Conc. (ppm) 11.87 BD 2.19 465000.00 96.17 85.82 39.23 1.40 61.08 7.17 0.05 BDDL 0.47 0.66 0.40 6.18 0.04 0.11 0.42 0.34 2.21 3.37 0.01 0.44Precision(%) 11.64 10.03 3.44 4.52 3.53 4.35 14.51 5.37 19.61 29.53

352
















OR23_1 Conc. (ppm)DLPrecision(%)



Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2389.41 32.42

0.36 BD 0.69 11.95 11.10 0.60 BD 0.58 26.84 0.61 4.61 BD BD BD0.12 2.55 0.12 0.08 1.11 0.09 0.01 0.03 0.04 0.02 0.02 0.01 0.01 0.01

20.48 9.67 12.88 13.80 30.22 22.91 9.75 14.92 10.1724.83 BD 0.71 0.12 BD BD BD BD 868.62 BD 0.41 BD BD BD0.09 2.29 0.16 0.08 1.11 0.09 0.01 0.04 0.04 0.02 0.03 0.02 0.01 0.01

26.60 10.61 33.72 20.74 25.470.15 BD 0.61 5.29 35.15 0.36 0.15 2.56 1.81 0.18 2.96 BD 0.02 BD0.07 2.86 0.13 0.07 1.07 0.06 0.01 0.03 0.03 0.01 0.03 0.02 0.01 0.01

38.33 11.00 12.37 6.27 27.60 35.26 26.79 7.13 12.23 10.70 23.710.84 BD 1.01 2.20 4.06 0.13 0.03 1.25 0.48 0.04 3.28 0.02 BD BD0.17 3.58 0.20 0.08 1.48 0.11 0.01 0.03 0.04 0.02 0.03 0.01 0.01 0.01

12.05 10.70 11.10 18.69 41.22 32.60 28.02 12.59 23.41 6.14 31.042.97 BD 0.63 9.88 4.42 0.41 0.04 1.48 0.46 0.06 12.28 0.08 0.02 BD0.09 2.93 0.18 0.07 1.47 0.09 0.01 0.02 0.04 0.02 0.02 0.01 0.01 0.016.94 12.62 3.43 16.33 17.68 23.39 6.34 12.35 13.97 3.36 12.76 32.771.27 BD 0.76 6.24 3.42 0.13 BD 0.13 0.39 0.09 6.34 0.05 0.03 BD0.13 3.18 0.17 0.07 0.97 0.12 0.01 0.05 0.05 0.01 0.03 0.01 0.01 0.018.69 426.75 10.36 5.58 18.03 41.25 20.79 12.36 13.94 4.95 18.25 19.482.06 2.64 1.74 5.02 7.24 1.75 0.82 125.67 0.43 0.23 5.19 0.08 0.01 BD0.12 2.55 0.14 0.06 1.20 0.12 0.01 0.04 0.03 0.02 0.04 0.01 0.00 0.019.58 39.25 7.15 7.15 11.70 12.79 48.86 19.36 13.78 9.77 6.47 12.40 30.461.37 BD 0.96 4.64 3.86 17.97 0.18 167.77 15.33 0.17 2.85 0.04 BD BD0.08 2.81 0.15 0.07 1.20 0.10 0.01 0.05 0.04 0.02 0.03 0.01 0.00 0.01

12.92 20.75 5.41 16.25 72.44 10.00 7.87 75.06 9.70 4.26 18.381.91 BD 0.70 14.61 3.64 1.52 0.28 3.95 3.62 0.13 4.22 BD 0.02 BD0.07 2.55 0.19 0.08 1.40 0.00 0.01 0.04 0.03 0.01 0.03 0.02 0.01 0.018.58 12.21 4.90 22.10 14.64 26.84 9.93 49.40 10.78 5.99 31.500.93 BD 1.22 34.97 4.79 122.81 0.31 3.55 2.28 2.49 7.47 BD 0.04 BD0.23 5.42 0.29 0.10 1.57 0.15 0.01 0.08 0.04 0.04 0.05 0.03 0.02 0.01

20.02 16.23 15.03 22.51 15.38 59.79 15.95 18.97 13.23 15.17 33.642.26 BD 0.81 78.87 7.38 0.63 BD 1.06 6.64 4.04 18.88 0.06 BD BD0.09 2.54 0.16 0.09 1.20 0.06 0.01 0.04 0.03 0.01 0.02 0.01 0.01 0.016.34 9.53 3.87 10.35 17.26 15.00 8.20 7.06 5.86 12.600.11 BD 0.74 1.66 BD BD BD BD 0.36 0.11 0.81 BD BD BD0.10 2.73 0.15 0.08 1.35 0.07 0.01 0.04 0.04 0.02 0.03 0.02 0.01 0.01

40.60 10.74 15.26 15.15 17.32 13.612.34 BD 0.75 41.15 7.68 0.72 0.46 5.52 49.34 2.07 8.47 0.06 0.07 BD0.08 2.64 0.18 0.05 1.22 0.06 0.01 0.03 0.04 0.02 0.03 0.01 0.01 0.015.88 11.09 6.26 10.91 10.85 29.80 11.70 7.50 4.25 5.85 15.66 15.280.45 BD 0.83 2.05 3.35 BD BD 1.14 0.39 0.05 5.45 0.05 BD BD0.11 2.89 0.17 0.07 1.79 0.09 0.01 0.05 0.05 0.02 0.04 0.01 0.01 0.01

15.44 10.42 7.27 23.56 66.40 12.64 20.79 5.10 14.610.70 1.10 0.63 BD 1.32 2.13 BD BD 0.08 0.16 9.07 0.55 BD BD0.08 2.55 0.14 0.07 1.19 0.08 0.01 0.05 0.04 0.01 0.02 0.01 0.01 0.01

14.98 86.44 10.78 41.31 22.74 28.56 10.28 18.63 12.468.89 6.00 0.65 653.56 17.70 BD BD BD 0.83 0.64 630.38 11.21 BD BD0.07 1.99 0.12 0.05 1.14 0.06 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.01

20.98 28.28 9.89 20.04 9.23 7.29 5.23 20.85 16.310.60 BD 0.58 13.80 3.77 BD BD BD 0.34 0.79 2.71 0.65 BD BD0.07 2.23 0.15 0.06 1.07 0.06 0.01 0.03 0.05 0.01 0.03 0.01 0.01 0.019.57 11.55 6.08 14.41 10.72 4.79 5.45 6.90

353

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Golden Mile Eastern Lode Oroya OR23_4-1 Conc. (ppm) 372.61 32.38 22.26 465000.00 745.61 172.58 28.10 16.71 347.71 17.16 13.73 4.28

DL 0.54 0.81 0.53 8.06 0.04 0.16 0.59 0.32 3.38 4.16 0.02 0.81Precision(%) 23.03 9.94 10.68 8.49 9.79 8.95 11.01 13.60 10.17 13.18 13.12 42.04

Golden Mile Eastern Lode Oroya OR23_4-2 Conc. (ppm) 105.28 1.55 26.78 465000.00 519.56 162.66 13.93 2.00 296.49 22.04 20.62 8.06DL 0.46 0.44 0.46 6.34 0.03 0.16 0.45 0.27 2.29 3.76 0.02 0.44Precision(%) 27.54 15.52 16.01 3.79 7.44 6.05 8.24 12.02 7.69 8.94 20.66 31.73

Golden Mile Eastern Lode Oroya OR25_1 Conc. (ppm) 22.65 1.47 20.30 465000.00 110.09 87.02 26.70 2.46 414.71 BD BD 0.71DL 0.45 0.64 0.39 7.56 0.04 0.16 0.47 0.31 1.81 3.61 0.02 0.47Precision(%) 10.35 21.89 12.22 3.64 7.02 4.87 5.71 10.02 9.69 26.71



Golden Mile Eastern Lode Oroya OR25_3-1 Conc. (ppm) 1510.02 119.57 447.96 465000.00 221.70 656.39 17.51 18.30 6584.79 16.00 26.26 BDDL 0.47 0.85 0.71 19.37 0.09 0.20 0.70 0.48 3.43 5.35 0.02 0.68Precision(%) 13.41 11.19 12.18 10.90 9.86 10.65 33.63 11.17 11.67 16.54 12.28





Golden Mile Eastern Lode Oroya OR3_1-3 Conc. (ppm) 17.39 BD 3.43 465000.00 41.40 36.32 6.94 1.43 58.03 53.42 0.08 BDDL 0.48 0.76 0.67 14.32 0.06 0.22 0.67 0.33 3.17 5.04 0.02 0.55Precision(%) 9.80 10.28 3.91 6.79 6.22 7.02 13.68 7.92 6.20 19.23

Golden Mile Eastern Lode Oroya OR3_2-1 Conc. (ppm) 8.36 BD 185.23 465000.00 19.44 54.88 379.96 4.34 2044.77 88.82 BD BDDL 0.27 0.52 0.52 8.16 0.02 0.16 0.35 0.23 2.18 3.32 0.02 0.39Precision(%) 10.91 16.03 3.44 4.58 6.51 6.07 12.97 6.46 5.03






Golden Mile Eastern Lode Oroya OR9_2-1 Conc. (ppm) 2951.62 14.85 7.95 465000.00 49.18 188.01 88.93 10.83 1972.22 4.59 29.96 BD

354

Sample NoOR23_4-1 Conc. (ppm)

DLPrecision(%)

OR23_4-2 Conc. (ppm)DLPrecision(%)
















OR9_2-1 Conc. (ppm)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2381.20 BD 1.47 164.17 2.72 100.78 0.05 1.15 0.29 0.49 139.60 2.89 0.32 0.140.11 2.98 0.16 0.12 1.33 0.09 0.01 0.07 0.06 0.01 0.03 0.02 0.01 0.01

10.60 9.06 10.25 23.65 12.31 35.20 29.55 14.56 7.94 10.55 10.13 17.06 16.730.64 BD 0.65 61.14 3.13 1.37 0.20 0.46 0.17 0.34 66.88 1.33 2.94 0.140.06 2.59 0.12 0.06 0.99 0.08 0.01 0.05 0.05 0.01 0.03 0.01 0.01 0.01

10.78 9.47 6.36 16.73 18.66 54.62 28.08 17.19 11.51 7.41 6.49 95.57 19.571.02 BD 0.54 20.57 11.39 0.43 BD BD 0.92 0.58 14.25 0.15 BD BD0.06 2.04 0.13 0.07 1.17 0.08 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.018.17 11.16 4.36 9.11 16.50 7.27 7.56 4.69 9.122.54 BD 0.91 119.77 56.33 51.91 0.75 0.18 1.61 0.72 69.50 0.60 0.18 0.100.10 2.23 0.17 0.06 1.21 0.07 0.01 0.04 0.05 0.02 0.03 0.01 0.01 0.016.48 9.07 4.94 6.28 6.73 19.47 21.50 6.65 5.58 4.68 5.80 11.99 13.082.21 BD 0.63 115.58 49.96 44.61 0.12 0.10 1.70 2.08 52.25 0.48 0.05 0.040.08 1.98 0.14 0.06 0.79 0.06 0.01 0.03 0.04 0.02 0.02 0.01 0.01 0.015.39 10.71 3.25 5.03 26.67 12.35 23.97 5.83 4.90 3.35 5.10 14.52 17.055.75 BD 2.89 27.14 25.60 112.26 0.10 4.18 1.67 0.81 16.41 0.19 1.30 0.160.12 3.78 0.20 0.07 1.32 0.07 0.01 0.05 0.06 0.02 0.03 0.01 0.01 0.01

25.72 36.22 10.78 13.93 11.80 14.40 15.40 13.82 8.74 9.76 14.13 85.17 14.561.54 BD 1.16 36.33 24.71 158.04 BD 8.27 3.18 1.93 11.72 0.15 0.29 0.240.20 6.93 0.40 0.17 4.12 0.25 0.03 0.12 0.10 0.05 0.10 0.03 0.02 0.03

21.49 21.12 17.85 27.67 16.65 27.21 18.55 14.73 17.19 21.62 20.05 20.161.83 BD 1.03 34.44 24.37 60.03 0.06 5.60 2.71 0.90 17.06 0.25 0.17 0.190.10 3.07 0.13 0.08 1.65 0.10 0.01 0.04 0.05 0.02 0.04 0.02 0.01 0.01

10.46 9.44 8.44 8.86 8.84 17.91 9.53 9.55 8.03 8.56 9.82 12.54 11.393.53 BD 1.29 5.16 72.85 37.05 0.06 3.10 4.20 0.14 3.57 0.31 0.07 0.080.13 2.67 0.19 0.10 1.10 0.06 0.01 0.05 0.06 0.02 0.02 0.01 0.01 0.016.43 7.81 5.68 6.44 10.62 16.28 10.09 9.99 12.42 4.61 9.94 12.42 12.83

16.19 2.91 1.27 104.03 120.64 12.83 0.61 9.24 38.78 0.64 96.66 0.27 0.25 0.100.10 2.58 0.18 0.08 1.08 0.09 0.01 0.05 0.03 0.02 0.03 0.01 0.01 0.01

11.33 36.55 7.03 3.77 6.23 6.31 11.28 3.92 8.70 5.52 4.65 8.42 8.24 10.024.70 BD 0.95 10.98 25.11 0.23 BD 0.07 3.25 2.14 4.22 0.06 BD BD0.13 3.14 0.19 0.07 1.30 0.09 0.01 0.04 0.05 0.01 0.03 0.01 0.01 0.01

11.04 9.88 4.51 7.51 25.45 31.36 10.87 4.95 5.42 15.7891.94 BD 0.85 50.61 433.53 5.56 0.01 BD 74.29 0.14 41.82 0.24 BD BD0.06 1.70 0.12 0.05 0.87 0.07 0.00 0.04 0.02 0.01 0.02 0.01 0.01 0.01

19.29 7.91 17.11 9.99 43.29 33.22 16.65 9.64 14.80 21.9919.02 BD 0.73 9.49 243.00 2.15 0.01 BD 14.44 0.04 32.31 0.09 BD BD0.05 1.63 0.13 0.05 0.67 0.10 0.00 0.04 0.03 0.02 0.02 0.01 0.01 0.01

27.38 10.31 19.84 9.16 70.51 30.39 29.67 30.37 34.66 21.99169.57 BD 1.53 134.22 2376.18 195.35 0.24 15.25 97.24 1.93 98.10 1.40 1.14 0.53

0.06 2.22 0.15 0.08 1.07 0.10 0.01 0.03 0.04 0.02 0.03 0.01 0.01 0.0117.42 10.98 12.45 26.31 16.47 17.72 11.77 13.62 9.12 13.17 13.91 26.05 11.65

131.58 BD 3.78 95.27 1316.26 696.75 0.63 19.88 120.61 5.65 69.30 2.77 0.73 0.270.15 3.74 0.21 0.15 2.26 0.18 0.01 0.08 0.08 0.02 0.05 0.02 0.01 0.01

17.23 10.30 14.89 16.15 10.82 39.69 15.39 17.81 11.66 14.72 12.59 17.53 18.040.66 2.11 0.58 17.29 21.08 2.75 0.60 5.79 0.59 0.06 12.09 0.11 0.25 0.100.06 1.80 0.14 0.05 1.18 0.08 0.01 0.05 0.02 0.01 0.03 0.01 0.01 0.019.92 34.67 11.45 4.61 7.46 7.71 6.23 4.76 11.46 13.96 4.38 10.00 6.21 7.762.97 BD 0.78 139.77 154.62 11.18 1.25 7.99 3.95 0.59 112.70 0.64 0.59 0.190.04 1.77 0.11 0.04 1.08 0.06 0.01 0.05 0.03 0.01 0.02 0.01 0.01 0.005.06 8.19 3.37 5.09 6.04 4.23 4.28 6.02 4.60 4.35 5.26 4.73 6.390.68 BD 0.64 37.67 19.19 3.27 0.53 7.73 0.56 0.15 12.18 0.14 0.36 0.14

355



Golden Mile Eastern Lode Oroya OR9_3-1 Conc. (ppm) 8.02 0.60 BD 465000.00 219.20 662.94 12.45 1.04 770.49 BD 0.11 BDDL 0.33 0.57 0.52 6.98 0.03 0.11 0.40 0.27 2.07 3.93 0.02 0.43Precision(%) 6.50 42.62 4.51 6.47 7.18 19.52 17.53 3.82 77.46





St Ives LD8122_108.0_1-1 Conc. (ppm) 24.22 16.10 0.74 465000.00 99.22 802.76 1.24 1.02 39.69 11.96 BD BDDL 0.33 0.54 0.53 6.51 0.05 0.18 0.58 0.30 11.80 2.72 0.02 0.44Precision(%) 9.24 10.77 29.08 3.92 4.78 4.08 20.81 17.17 12.09 11.21

St Ives LD8122_108.0_1-2 Conc. (ppm) 398.31 51.90 0.73 465000.00 356.37 123.46 1.64 1.24 31.47 49.32 208.42 BDDL 0.47 0.73 0.50 9.23 0.05 0.20 0.57 0.30 10.02 2.22 0.01 0.43Precision(%) 20.88 16.01 27.99 4.15 6.61 5.58 16.29 16.08 14.12 7.03 22.84

St Ives LD8122_108.0_1-3 Conc. (ppm) 457.19 8.82 BD 465000.00 471.99 1278.39 BD 1.07 68.93 15.25 0.73 BDDL 0.50 0.66 0.51 10.32 0.05 0.19 0.55 0.38 9.00 2.09 0.02 0.48Precision(%) 20.57 13.22 3.87 7.09 4.20 18.78 10.15 8.67 16.94

St Ives LD8122_108.0_2-1 Conc. (ppm) 1179.24 90.41 BD 465000.00 376.22 768.91 3.48 1.63 30.99 5.26 8.77 BDDL 0.43 0.62 0.58 22.01 0.05 0.18 0.68 0.52 10.10 3.34 0.02 0.58Precision(%) 18.12 12.95 3.89 7.51 4.21 12.00 36.53 13.55 25.62 41.84

St Ives LD7113A_135.5_1-1 Conc. (ppm) 6.04 BD 0.50 465000.00 948.34 393.48 BD 0.91 2.95 16.80 BD BDDL 0.30 0.62 0.37 5.31 0.05 0.17 0.43 0.27 0.40 3.99 0.02 0.42Precision(%) 6.61 28.99 4.10 4.06 3.72 17.10 8.04 10.58

St Ives LD7113A_135.5_1-2 Conc. (ppm) 7.79 0.64 56.48 465000.00 16.27 27.73 223.08 1.73 14.28 67.77 BD 16.10DL 0.45 0.50 0.45 6.73 0.06 0.17 0.56 0.41 0.47 3.65 0.01 0.53Precision(%) 6.10 36.36 26.61 3.78 3.99 5.32 33.84 14.23 4.36 4.67 9.95

St Ives LD7113A_135.5_2-1 Conc. (ppm) 6.88 BD BD 465000.00 70.68 157.30 BD 0.92 8.06 105.04 BD BDDL 0.40 0.64 0.45 6.72 0.05 0.11 0.47 0.30 0.43 4.03 0.02 0.51Precision(%) 6.67 3.94 9.62 3.63 20.13 5.64 5.68

St Ives LD7113A_135.5_2-2 Conc. (ppm) 6.86 BD BD 465000.00 410.63 499.92 0.93 0.72 73.98 79.39 BD BDDL 0.51 0.61 0.55 7.80 0.05 0.14 0.43 0.37 0.50 3.66 0.01 0.50Precision(%) 7.07 3.96 3.75 4.70 22.17 24.67 5.93 4.60

St Ives LD7113A_135.5_3-1 Conc. (ppm) 20.26 19.42 6.56 465000.00 619.32 722.48 46.07 4.77 61.88 47.15 BD BDDL 0.47 0.60 0.52 10.60 0.07 0.18 0.49 0.35 0.48 4.44 0.01 0.45Precision(%) 8.26 16.25 14.26 3.54 5.53 4.13 28.53 15.31 6.19 5.73

St Ives LD7113A_135.5_3-2 Conc. (ppm) 6.43 BD 0.63 465000.00 206.77 1020.34 449.85 2.17 39.01 40.45 BD BDDL 0.51 0.67 0.46 18.00 0.05 0.13 0.47 0.28 0.42 3.96 0.01 0.42Precision(%) 8.94 31.30 3.58 8.10 5.75 23.00 15.16 10.14 9.75

St Ives CD2949_169.45_3-2 Conc. (ppm) 5.87 BD BD 465000.00 15035.37 11.76 BD 1.07 31.09 33.30 BD BDDL 0.36 0.49 0.36 0.00 0.00 0.12 0.34 0.21 0.35 3.94 0.02 0.45

356








LD8122_108.0_1-1 Conc. (ppm)DLPrecision(%)




LD7113A_135.5_1-1 Conc. (ppm)DLPrecision(%)






CD2949_169.45_3-2 Conc. (ppm)DL


14.71 9.23 6.56 9.76 8.04 5.80 6.15 15.05 9.92 5.72 10.24 6.82 7.190.45 BD 0.62 9.69 18.21 1.34 0.31 9.44 1.78 0.05 7.54 0.04 0.37 0.230.07 2.28 0.14 0.06 0.81 0.06 0.01 0.04 0.04 0.01 0.02 0.01 0.00 0.01

10.53 10.86 5.86 6.63 10.04 6.88 5.79 9.23 16.31 4.63 21.28 6.37 5.610.30 BD 0.56 8.71 18.76 0.57 BD BD 0.55 BD 4.77 0.08 BD BD0.07 1.83 0.14 0.04 1.26 0.10 0.01 0.03 0.03 0.02 0.02 0.01 0.01 0.00

15.65 11.99 5.19 7.61 14.77 10.27 5.25 12.170.41 BD 0.71 10.25 19.43 2.43 BD BD 0.51 1.47 4.53 0.07 BD 0.000.09 2.23 0.16 0.07 1.26 0.07 0.01 0.03 0.03 0.01 0.02 0.01 0.01 0.01

13.02 10.34 5.03 7.77 15.46 9.50 6.73 5.48 13.62 168.400.24 BD 0.68 3.29 9.69 3.97 BD BD 0.22 0.44 2.36 0.03 BD BD0.06 2.56 0.16 0.06 1.00 0.07 0.00 0.04 0.03 0.01 0.03 0.01 0.01 0.01

18.03 11.36 21.30 18.80 38.24 15.37 7.22 18.71 31.050.97 0.07 0.67 24.46 17.70 2.51 0.58 7.08 0.44 0.14 12.50 0.16 0.39 0.150.08 2.11 0.12 0.06 1.15 0.07 0.01 0.06 0.03 0.01 0.02 0.01 0.01 0.018.23 1093.29 9.30 5.10 8.97 6.96 6.23 5.18 11.15 14.29 4.40 8.51 6.29 7.560.73 BD 0.73 7.69 12.46 1.09 0.71 7.54 0.66 0.05 20.47 0.07 0.23 0.080.05 2.22 0.13 0.06 1.21 0.08 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.018.67 9.22 4.17 7.42 9.69 37.50 4.39 9.31 15.34 3.85 12.44 6.61 9.460.18 BD 0.52 BD 1.71 13.48 BD 0.17 0.04 BD 1.41 5.76 BD BD0.07 2.17 0.15 0.06 1.25 0.06 0.01 0.03 0.03 0.01 0.04 0.01 0.01 0.00

19.91 12.51 32.31 12.28 15.90 46.69 7.64 7.620.34 BD 0.68 0.27 2.69 36.66 0.04 0.67 0.09 0.02 1.48 11.31 0.51 1.280.09 2.31 0.16 0.06 1.30 0.08 0.01 0.04 0.04 0.01 0.03 0.01 0.01 0.00

17.50 11.22 18.29 21.83 17.99 21.54 18.96 29.23 26.68 6.73 6.19 35.31 21.500.09 BD 0.49 0.24 1.13 2.05 BD 1.56 BD BD 0.65 2.20 BD BD0.07 1.99 0.15 0.07 0.81 0.10 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.01

38.49 12.98 22.37 35.10 19.18 15.93 291.13 10.73 9.290.19 BD 0.81 0.64 3.24 15.33 0.02 4.54 0.37 BD 3.74 8.46 0.03 0.050.10 1.80 0.12 0.05 1.20 0.11 0.01 0.02 0.05 0.01 0.02 0.01 0.00 0.01

25.95 8.61 15.53 19.59 14.70 31.35 12.14 34.32 8.93 9.68 31.63 36.93BD BD 0.51 BD BD BD BD BD BD BD BD 0.04 BD BD

0.07 2.49 0.10 0.07 1.48 0.08 0.01 0.04 0.03 0.01 0.02 0.01 0.01 0.009.68 42.71

0.29 BD 0.58 0.15 359.24 BD BD 1478.90 0.15 BD 1.78 9.58 BD BD0.09 2.61 0.10 0.05 1.29 0.08 0.01 0.03 0.02 0.01 0.03 0.01 0.01 0.01

21.70 9.01 21.59 5.03 13.92 24.94 9.26 8.45 372.80BD BD 0.60 BD 69.27 BD BD BD BD BD BD 0.18 BD BD

0.09 2.34 0.12 0.07 1.28 0.08 0.01 0.05 0.03 0.01 0.03 0.01 0.01 0.009.63 6.15 9.02

BD BD 0.64 BD 601.98 BD BD 0.94 0.05 BD 0.08 1.45 BD BD0.08 2.87 0.11 0.10 1.64 0.06 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.00

9.11 4.86 18.47 68.72 19.74 14.500.59 BD 0.58 0.30 30.08 0.20 BD 0.05 0.58 BD 5.10 30.54 BD BD0.07 2.38 0.13 0.06 1.26 0.09 0.01 0.03 0.03 0.01 0.03 0.01 0.01 0.01

11.39 10.19 15.50 8.70 25.76 34.22 10.61 7.60 9.771.21 BD 0.43 BD 127.01 BD 0.02 BD 0.18 BD 2.27 65.70 BD BD0.09 2.56 0.11 0.08 1.32 0.11 0.01 0.02 0.04 0.01 0.02 0.01 0.01 0.01

27.32 14.60 11.13 103.63 24.65 43.33 25.270.14 BD 0.44 0.11 5.99 BD BD BD BD BD 1.11 1.73 BD BD0.08 2.12 0.10 0.06 1.02 0.08 0.01 0.03 0.02 0.01 0.03 0.01 0.00 0.00

357

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95Precision(%) 8.44 9.08 7.70 12.36 17.16 10.73 9.58

St Ives LD8122_201.0_1-1 Conc. (ppm) 21.19 BD BD 465000.00 105.03 1078.84 4.52 1.02 125.89 9.22 0.60 BDDL 0.39 0.59 0.57 6.37 0.03 0.10 0.54 0.35 16.78 3.63 0.02 0.46Precision(%) 21.98 3.74 8.64 5.11 27.22 17.89 7.04 17.12 24.67

St Ives LD8122_201.0_2-1 Conc. (ppm) 6.44 BD BD 465000.00 786.62 1392.77 10.01 0.77 113.88 62.88 BD BDDL 0.43 0.72 0.56 7.31 0.06 0.11 0.52 0.35 13.79 3.23 0.02 0.45Precision(%) 7.22 3.67 4.31 4.06 29.83 22.72 6.58 4.53



St Ives LD8122_201.0_2-4 Conc. (ppm) 43.56 0.60 BD 465000.00 736.42 1683.23 0.50 0.88 63.53 12.18 4.20 BDDL 0.51 0.58 0.54 9.04 0.05 0.15 0.49 0.41 10.45 3.35 0.02 0.46Precision(%) 52.43 87.46 3.87 4.87 4.98 43.05 23.72 8.66 14.27 52.38

St Ives LD8122_201.0_3-1 Conc. (ppm) 6.99 BD 0.48 465000.00 55.54 420.10 0.97 0.99 50.67 39.36 BD BDDL 0.45 0.68 0.47 6.70 0.06 0.25 0.52 0.25 10.90 3.17 0.00 0.50Precision(%) 16.25 39.49 3.79 15.81 10.97 26.32 14.95 9.88 6.28

St Ives LD8122_201.0_3-2 Conc. (ppm) 7.36 6.79 BD 465000.00 112.04 1373.47 BD 1.19 42.57 9.76 BD BDDL 0.55 0.72 0.61 6.24 0.06 0.15 0.65 0.28 10.03 2.88 0.02 0.52Precision(%) 7.45 27.76 3.74 4.22 3.40 16.73 10.54 13.38

St Ives LD7113A_310.4_1-1 Conc. (ppm) 7.84 1.43 28.56 465000.00 231.88 675.09 1.45 2.15 23.28 9.06 0.05 BDDL 0.45 0.62 0.65 7.54 0.06 0.25 0.63 0.39 7.11 3.87 0.03 0.56Precision(%) 6.85 27.03 19.18 4.06 4.31 3.87 25.38 14.88 13.64 18.42 31.11


St Ives LD7113A_310.4_1B-1 Conc. (ppm) 37.17 133.48 5.90 465000.00 194.58 959.91 1.60 2.21 15.23 14.28 0.07 BDDL 0.59 0.65 0.65 8.89 0.09 0.20 0.74 0.38 8.42 3.00 0.03 0.50Precision(%) 16.00 18.04 19.94 4.31 8.94 4.68 21.75 18.66 22.07 10.62 28.94

St Ives LD7113A_310.4_1B-2 Conc. (ppm) 7.69 7.23 0.67 465000.00 912.07 1669.78 BD 0.96 21.23 12.92 BD BDDL 0.43 0.65 0.53 9.62 0.05 0.14 0.67 0.43 7.99 3.55 0.01 0.55Precision(%) 7.23 20.35 33.41 4.12 6.83 4.01 44.96 23.27 15.11 12.45

St Ives LD7113A_310.4_1B-3 Conc. (ppm) 151.25 241.89 41.55 465000.00 212.31 643.00 40.12 6.73 15.40 18.05 0.41 BDDL 0.69 0.63 0.68 10.94 0.05 0.21 0.96 0.44 6.46 3.27 0.00 0.61Precision(%) 5.77 5.37 4.82 3.61 4.21 3.43 12.36 7.47 18.06 9.13 23.96

St Ives LD7113A_310.4_1B-4 Conc. (ppm) 18.54 33.74 4.73 465000.00 651.83 1069.01 13.17 1.47 25.74 29.57 BD 8.89DL 0.50 0.60 0.47 9.06 0.06 0.21 0.64 0.43 6.62 3.26 0.02 0.60Precision(%) 12.24 15.01 18.44 3.74 6.12 8.12 24.55 16.75 11.42 7.69 50.93

St Ives LD70026A_317.15_1-1 Conc. (ppm) 5.19 0.61 BD 465000.00 652.98 1496.45 BD 0.83 10.37 15.58 BD BDDL 0.31 0.60 0.43 7.16 0.05 0.14 0.43 0.26 0.38 4.60 0.02 0.43Precision(%) 6.88 40.10 3.66 3.38 3.50 18.50 4.63 13.36

St Ives LD70026A_317.15_1-2 Conc. (ppm) 6.01 BD BD 465000.00 198.28 159.27 1.69 0.84 0.99 5.11 BD BDDL 0.48 0.58 0.47 7.25 0.06 0.15 0.52 0.32 0.47 4.91 0.01 0.48Precision(%) 7.01 4.18 8.37 5.01 21.97 20.14 20.07 37.13

St Ives LD70026A_317.15_1-3 Conc. (ppm) 117.62 552.36 0.56 465000.00 2099.21 695.37 6.98 4.99 3.34 11.53 BD BDDL 0.65 0.66 0.54 16.13 0.05 0.23 0.58 0.44 0.42 5.08 0.01 0.53Precision(%) 8.01 8.76 37.67 5.39 8.09 5.81 12.22 9.08 9.29 19.67

St Ives LD70026A_317.15_2-1 Conc. (ppm) 42.11 BD 158.49 465000.00 4017.65 5543.48 276647.96 147.28 2262.03 226.98 BD BDDL 1.41 2.12 1.26 20.59 0.10 0.52 1.72 1.22 1.36 14.48 0.06 1.59Precision(%) 20.10 16.52 8.49 16.00 15.73 11.00 13.57 13.98 9.64

358











LD7113A_310.4_1B-1 Conc. (ppm)DLPrecision(%)








Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23830.55 12.17 31.38 19.66 18.77 21.08

BD BD 0.59 BD 0.94 BD BD 0.50 BD BD 1.31 0.58 0.03 0.020.07 2.38 0.15 0.07 0.88 0.09 0.01 0.03 0.03 0.02 0.03 0.01 0.01 0.01

12.15 42.90 33.27 11.41 20.39 26.35 37.620.08 BD 0.70 BD 5.17 BD BD BD 0.06 BD 0.54 1.80 BD BD0.07 2.09 0.15 0.06 1.37 0.11 0.01 0.03 0.04 0.01 0.03 0.01 0.01 0.00

38.85 9.90 14.12 31.81 10.41 7.56BD BD 0.66 BD BD 1.69 1.72 0.74 0.11 BD 1.31 1.34 0.28 0.14

0.08 1.85 0.13 0.06 1.07 0.07 0.01 0.05 0.04 0.02 0.03 0.01 0.00 0.0110.22 30.25 39.63 18.74 36.08 7.72 8.59 21.04 26.49

0.69 BD 0.66 0.17 46.42 70.65 0.18 0.08 0.87 BD 14.16 60.00 0.89 0.330.09 2.65 0.17 0.08 1.26 0.13 0.01 0.00 0.05 0.01 0.03 0.01 0.01 0.01

15.04 12.52 23.01 8.83 16.57 12.06 21.57 32.41 5.77 6.87 33.34 29.69BD BD 0.76 BD 1.03 BD BD 1.94 BD BD 0.29 0.38 0.10 0.09

0.06 2.39 0.14 0.07 0.94 0.09 0.01 0.05 0.03 0.01 0.03 0.01 0.01 0.018.88 42.79 54.62 30.73 25.28 54.27 52.12

BD BD 0.66 BD 36.84 BD BD BD BD BD 0.41 0.60 BD BD0.08 2.41 0.15 0.04 0.99 0.10 0.01 0.03 0.02 0.01 0.03 0.02 0.01 0.01

10.59 11.02 14.36 15.68BD BD 0.62 BD BD 1.29 BD BD BD BD 0.27 0.39 BD BD

0.10 2.52 0.16 0.06 1.34 0.08 0.01 0.05 0.04 0.01 0.03 0.00 0.01 0.0111.47 25.01 19.16 15.53

0.14 BD 0.87 BD 0.79 BD BD BD 0.08 BD 0.34 0.28 BD BD0.07 2.30 0.15 0.10 1.05 0.05 0.01 0.04 0.04 0.02 0.03 0.01 0.01 0.01

29.28 8.93 57.81 49.55 12.75 7.170.47 BD 0.73 0.17 13.90 4.46 BD BD 0.38 0.03 8.09 21.89 BD BD0.09 2.51 0.22 0.07 1.14 0.13 0.01 0.06 0.05 0.01 0.03 0.01 0.01 0.01

15.10 14.03 21.91 9.71 13.25 26.70 26.12 7.64 7.93BD BD 0.77 0.07 4.24 0.24 BD BD BD 0.02 7.07 3.24 BD BD

0.08 2.14 0.17 0.04 1.65 0.04 0.01 0.03 0.05 0.01 0.04 0.02 0.01 0.0010.33 31.71 21.76 22.41 32.06 12.56 10.57

BD BD 0.73 BD 2.17 BD BD BD BD BD 1.74 1.00 BD BD0.08 2.81 0.14 0.09 1.13 0.06 0.01 0.06 0.02 0.02 0.03 0.01 0.01 0.00

10.14 31.98 22.12 17.350.64 BD 0.91 0.47 31.38 3.30 BD 0.12 0.77 0.09 54.70 39.47 BD BD0.09 2.36 0.16 0.07 1.45 0.11 0.01 0.03 0.05 0.02 0.03 0.02 0.01 0.01

10.81 9.04 11.42 6.33 13.02 16.93 11.83 11.71 4.80 4.08BD BD 0.66 BD 29.11 BD BD BD 0.16 BD 11.90 8.78 BD BD

0.10 2.60 0.12 0.07 1.39 0.10 0.01 0.04 0.02 0.01 0.02 0.01 0.01 0.019.24 8.98 17.07 7.63 7.85

BD BD 0.68 BD BD BD BD BD 0.13 BD 0.06 0.37 BD BD0.09 2.65 0.10 0.06 1.37 0.07 0.01 0.03 0.02 0.01 0.03 0.01 0.01 0.00

8.55 24.94 23.79 7.58BD BD 0.65 BD BD BD BD 0.03 BD BD 0.06 0.22 BD BD

0.10 2.27 0.14 0.08 1.45 0.05 0.01 0.02 0.03 0.01 0.03 0.01 0.01 0.0110.30 44.69 21.14 7.51

0.25 BD 0.94 0.45 6.86 36.76 BD 3.85 0.34 0.18 4.47 11.77 BD BD0.13 2.39 0.13 0.06 1.54 0.09 0.01 0.04 0.02 0.02 0.03 0.01 0.01 0.01

26.27 8.09 11.35 13.28 8.75 8.69 17.69 10.01 5.77 7.66119.16 BD 2.01 2.68 212.32 0.25 BD 0.15 0.62 1.03 13.63 314.68 BD BD

0.30 7.49 0.35 0.24 4.55 0.14 0.03 0.12 0.09 0.03 0.06 0.02 0.02 0.0223.31 10.96 14.14 28.81 33.93 43.34 20.17 14.93 20.40 23.14

359

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95St Ives LD70026A_317.15_2-2 Conc. (ppm) 56.62 BD 1830.79 465000.00 530.34 677.10 405802.34 389.79 223.55 410.43 BD BD

DL 1.27 2.14 1.51 28.68 0.21 0.44 0.00 1.13 1.56 16.34 0.05 1.99Precision(%) 22.50 24.68 4.16 28.97 27.17 11.67 14.49 33.84 7.06

St Ives CD10095W2_386.0_1C Conc. (ppm) 62.20 40.33 0.86 465000.00 473.28 752.33 1.73 3.89 4.67 4.00 BD BDDL 0.72 0.66 0.56 6.43 0.04 0.22 0.63 0.35 2.56 3.23 0.03 0.78Precision(%) 9.48 9.22 35.10 4.12 7.28 4.24 18.09 9.65 22.27 33.53

St Ives CD10095W2_386.0_1R Conc. (ppm) 10.22 BD BD 465000.00 1250.55 1177.76 332.49 1.70 7.65 14.78 BD BDDL 0.34 0.85 0.39 6.94 0.04 0.06 0.53 0.29 2.24 4.13 0.01 0.53Precision(%) 6.28 3.79 6.15 3.83 23.58 14.94 13.16 12.07

St Ives CD10095W2_386.0_2C Conc. (ppm) 2598.80 47.25 1.14 465000.00 940.45 1978.35 30.54 1.76 10.37 6.68 0.33 BDDL 0.53 0.74 0.41 5.88 0.04 0.12 0.46 0.24 2.24 3.23 0.02 0.59Precision(%) 13.56 10.82 38.17 3.31 5.50 4.26 17.37 14.23 9.27 21.26 12.64

St Ives CD10095W2_386.0_2R Conc. (ppm) 9.63 5.14 BD 465000.00 401.67 468.93 BD 1.38 BD 4.56 BD BDDL 0.35 0.62 0.40 5.97 0.05 0.14 0.49 0.23 2.22 2.88 0.01 0.61Precision(%) 6.02 33.18 3.88 5.65 4.46 11.91 26.10

St Ives CD10095W2_386.0_3C Conc. (ppm) 11.33 6.37 BD 465000.00 1147.86 2505.23 0.88 0.98 7.91 11.36 0.08 BDDL 0.48 0.78 0.43 6.79 0.03 0.18 0.48 0.30 2.19 2.84 0.01 0.72Precision(%) 8.15 14.86 3.81 6.13 4.29 26.12 19.52 11.81 11.59 67.39

St Ives CD10095W2_386.0_3R Conc. (ppm) 113.71 20.72 1.14 465000.00 733.98 1083.31 0.70 3.66 4.45 7.90 0.07 BDDL 0.39 0.71 0.39 6.76 0.04 0.12 0.45 0.19 2.08 2.54 0.02 0.46Precision(%) 15.05 15.92 42.94 3.71 7.73 5.61 29.25 24.25 20.10 14.37 34.61

St Ives LD7113A_42.8_1-1 Conc. (ppm) 3510.82 BD 2400.64 465000.00 18.68 388.17 28276.55 12266.49 BD 144.92 0.61 BDDL 3.11 5.16 4.48 74.95 0.48 1.51 9.85 2.70 4.26 47.84 0.22 5.45Precision(%) 23.64 14.87 15.45 24.85 17.32 35.64 20.54 39.84 27.97

St Ives CD10095W2_423.0_1-1 Conc. (ppm) 20.36 BD 0.49 465000.00 13687.25 4.46 0.39 0.82 5.03 15.41 56.98 BDDL 0.28 0.48 0.29 6.58 0.18 0.12 0.36 0.33 1.36 3.11 0.01 0.54Precision(%) 15.19 27.07 4.02 3.81 5.91 37.50 19.17 12.35 9.56 20.06

St Ives CD10095W2_423.0_1-2 Conc. (ppm) 648.70 6.71 54.88 465000.00 7269.80 10.37 141.60 9.75 91.49 9.32 8.11 BDDL 0.51 0.51 0.34 8.32 0.13 0.13 0.51 0.26 1.37 3.10 0.01 0.44Precision(%) 11.54 10.26 7.44 4.33 3.84 6.96 41.50 9.05 5.79 14.83 19.83

St Ives CD10095W2_423.0_3-1 Conc. (ppm) 19.37 BD 21.76 465000.00 6811.16 8.10 BD 0.93 159.06 4.18 0.19 BDDL 0.32 0.80 0.37 5.22 0.05 0.19 0.43 0.19 1.54 3.52 0.01 0.50Precision(%) 19.33 74.27 15.87 4.20 3.94 4.52 17.11 3.76 34.49 15.09

St Ives CD10095W2_423.0_3-2 Conc. (ppm) 6412.15 7.64 75.70 465000.00 6787.52 11.24 5.85 3.63 266.61 9.93 35.90 BDDL 0.34 0.56 0.32 14.26 0.05 0.11 0.39 0.16 1.72 2.69 0.01 0.50Precision(%) 14.10 13.33 16.99 4.72 4.43 5.92 37.43 11.29 4.10 12.51 26.91


St Ives LD7113A_43.1_1-2 Conc. (ppm) 1237.95 641.10 833.03 465000.00 159.53 959.84 BD 6.09 139.57 31.26 7.30 BDDL 0.99 2.51 1.45 35.77 0.19 0.48 2.15 1.30 19.48 10.00 0.05 1.60Precision(%) 23.89 20.21 16.52 21.12 27.43 25.07 33.69 23.06 27.36 20.89




St Ives LD8122_53.2_3-1 Conc. (ppm) 60.72 16.56 8.99 465000.00 4957.66 201.66 3.33 2.65 196.99 20.74 67.11 BD

360

Sample NoLD70026A_317.15_2-2 Conc. (ppm)

DLPrecision(%)

CD10095W2_386.0_1C Conc. (ppm)DLPrecision(%)

CD10095W2_386.0_1R Conc. (ppm)DLPrecision(%)






CD10095W2_423.0_1-1 Conc. (ppm)DLPrecision(%)









LD8122_53.2_3-1 Conc. (ppm)

Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23891.02 BD 2.91 0.90 15.23 0.55 0.58 0.45 BD 0.10 3.55 13.40 BD BD0.31 8.97 0.52 0.26 5.54 0.32 0.02 0.08 0.09 0.05 0.10 0.05 0.02 0.035.61 10.95 30.35 30.71 47.74 44.52 31.20 37.53 16.07 25.30 237.75

BD 0.85 0.77 BD 6.45 5.46 BD 1.01 0.17 BD 1.84 2.93 BD BD0.11 3.01 0.16 0.09 1.74 0.10 0.01 0.05 0.02 0.02 0.03 0.01 0.01 0.01

136.69 10.33 15.43 10.59 11.64 18.10 7.89 6.114.19 BD 0.58 0.17 5.66 1.30 BD BD BD BD 1.12 1.48 BD BD0.08 3.16 0.13 0.07 1.50 0.08 0.01 0.05 0.05 0.01 0.02 0.02 0.01 0.01

31.10 11.77 35.53 34.51 23.25 12.31 12.66BD BD 0.87 1.07 4.88 2.95 0.20 11.79 0.19 0.03 3.96 5.06 0.20 0.16

0.09 2.83 0.13 0.07 1.12 0.07 0.01 0.03 0.05 0.01 0.02 0.01 0.01 0.019.07 11.14 14.89 17.51 13.24 12.96 27.49 37.00 7.93 6.93 13.43 14.26

BD BD 0.43 BD BD 0.10 BD BD BD BD 0.05 0.04 BD BD0.09 2.44 0.13 0.08 1.50 0.08 0.01 0.03 0.04 0.01 0.02 0.01 0.01 0.01

13.35 47.47 27.67 26.53 300.25BD BD 0.47 BD 0.78 0.57 BD 0.07 BD BD 0.92 1.03 BD BD

0.08 2.88 0.13 0.08 1.27 0.08 0.01 0.06 0.04 0.01 0.03 0.01 0.01 0.0113.43 71.34 19.11 67.69 8.83 5.94

0.21 BD 0.62 0.09 0.97 8.58 0.02 0.64 0.05 BD 1.58 1.37 BD BD0.08 2.39 0.12 0.06 1.53 0.08 0.01 0.06 0.04 0.01 0.03 0.01 0.01 0.01

43.23 10.41 36.26 62.44 25.41 34.79 15.94 50.36 8.77 9.9453.29 206.87 5.92 3.86 3915.45 4.91 0.12 18.64 BD 0.09 5.79 5046.12 BD 0.401.00 26.77 1.37 0.87 14.12 0.74 0.09 0.31 0.27 0.14 0.29 0.08 0.04 0.05

18.93 27.16 21.01 27.99 31.88 20.39 42.92 24.88 85.74 25.85 29.68 24.61BD BD 0.36 BD BD 0.59 0.13 BD BD BD 1.08 0.36 1.57 0.77

0.07 2.41 0.10 0.07 1.12 0.04 0.01 0.03 0.03 0.01 0.02 0.01 0.00 0.0113.07 19.43 39.04 9.88 11.56 16.23 16.76

4.63 BD 0.52 1.37 12.53 13.27 0.19 0.13 BD 0.02 8.15 13.50 0.32 0.130.08 2.46 0.13 0.06 1.38 0.06 0.01 0.03 0.04 0.01 0.02 0.01 0.00 0.00

12.65 12.46 7.61 13.84 15.78 14.79 20.58 26.94 9.78 7.13 23.00 15.76BD BD 0.25 0.10 BD BD BD BD BD BD 0.84 0.51 BD 0.00

0.07 2.49 0.16 0.05 1.18 0.07 0.01 0.04 0.04 0.01 0.02 0.01 0.01 0.0124.26 26.99 9.08 9.45 469.35

0.08 BD 1.38 0.85 BD 0.60 3.31 1.34 0.04 BD 5.37 2.86 1.26 1.240.07 2.20 0.13 0.06 1.41 0.03 0.01 0.03 0.03 0.01 0.03 0.02 0.01 0.01

46.32 12.10 11.83 15.82 19.89 14.37 43.53 7.32 5.73 18.77 18.972.77 BD 0.88 0.84 14.07 2.35 0.26 0.20 0.08 BD 1.93 30.13 0.17 0.040.11 3.22 0.15 0.07 1.73 0.09 0.01 0.04 0.03 0.02 0.03 0.01 0.01 0.01

10.90 8.94 13.05 9.18 16.20 13.98 17.16 23.94 8.05 8.18 8.63 17.020.78 BD 3.56 2.65 5.67 2.73 2.26 1.07 BD BD 4.96 16.51 0.24 0.170.35 7.76 0.44 0.19 4.00 0.32 0.04 0.09 0.11 0.02 0.11 0.04 0.03 0.03

49.55 17.91 34.73 40.60 18.63 18.69 22.03 17.06 43.72 22.30 21.780.45 BD 0.72 0.40 31.75 0.74 0.08 0.21 0.14 BD 3.55 17.63 0.16 0.070.10 2.42 0.16 0.07 1.50 0.08 0.02 0.03 0.03 0.01 0.03 0.01 0.00 0.01

13.56 9.59 16.36 6.60 18.01 24.35 14.52 19.61 4.73 5.60 8.86 15.760.31 BD 1.00 0.67 18.11 74.40 0.06 0.53 0.22 0.02 9.81 60.35 0.20 0.070.12 2.29 0.16 0.07 1.32 0.11 0.01 0.05 0.03 0.01 0.03 0.02 0.01 0.01

17.91 8.25 8.72 7.15 8.15 15.40 10.00 14.19 34.26 5.23 3.97 10.31 11.690.15 BD 0.71 0.22 8.04 0.18 BD BD BD BD 2.03 20.02 0.02 0.010.10 2.33 0.14 0.05 1.22 0.09 0.01 0.04 0.03 0.01 0.03 0.01 0.01 0.00

27.88 9.92 18.61 11.65 25.58 8.71 7.94 70.60 39.830.14 BD 0.98 0.26 11.08 0.55 BD 100.95 0.16 BD 1.29 17.22 0.14 0.10

361




362





25.15 8.07 16.25 9.63 27.33 12.70 14.43 6.24 5.53 9.39 15.100.28 BD 2.99 0.18 5.29 0.49 BD 0.23 0.08 BD 2.76 11.12 0.07 0.020.08 2.51 0.14 0.06 1.09 0.11 0.01 0.02 0.03 0.02 0.02 0.01 0.01 0.01

26.16 65.42 20.04 13.39 22.56 14.51 29.79 10.54 5.34 11.83 22.110.17 1.17 0.72 0.29 18.32 0.25 BD 0.67 0.16 BD 1.12 30.25 0.02 BD0.10 2.30 0.13 0.04 1.26 0.09 0.01 0.03 0.02 0.01 0.03 0.01 0.01 0.01

30.43 77.97 9.90 15.68 18.91 42.40 16.98 18.99 9.95 15.60 26.76

363

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75

New Celebration 1250_12-4_1A Conc. (ppm) 578.78 73.11 205.24 723000.00 73.83 149.93 BD 155.10 BDDL 0.74 1.35 0.70 14.93 0.12 0.30 1.27 0.47 1.03Precision(%) 6.59 5.54 2.78 2.68 2.79 2.93 15.16

New Celebration 1250_12-4_1B Conc. (ppm) 448.44 106.51 168.25 723000.00 77.25 157.88 BD 185.76 BDDL 0.68 1.32 0.85 14.05 0.14 0.37 1.31 0.46 1.03Precision(%) 4.34 8.59 2.83 2.65 2.83 2.95 8.66

New Celebration 1250_12-4_3-1 Conc. (ppm) 504.25 714.05 95.96 723000.00 72.92 133.63 BD 129.24 1.66DL 0.61 1.22 0.78 12.38 0.10 0.35 1.19 0.64 1.04Precision(%) 11.78 4.71 3.50 2.71 2.77 3.03 10.34 26.51

New Celebration 1250_12-4_3-2 Conc. (ppm) 322.91 1349.07 118.97 723000.00 72.31 132.82 BD 159.47 BDDL 0.99 1.33 1.11 26.47 0.10 0.40 1.37 0.67 1.36Precision(%) 3.23 5.56 3.13 2.82 2.98 3.18 3.51

New Celebration 1250_12-4_3-3 Conc. (ppm) 241.35 723.38 81.72 723000.00 70.22 130.09 BD 134.19 1.08DL 0.81 1.48 0.82 38.23 0.13 0.41 1.15 0.51 0.91Precision(%) 3.63 4.81 3.77 2.97 3.17 3.25 5.76 37.32



New Celebration 133565_1-2 Conc. (ppm) 202.15 623.26 23.04 723000.00 8.40 226.98 1.57 51.62 1.47DL 1.41 2.25 1.31 20.91 0.17 0.76 2.24 0.91 1.45Precision(%) 9.72 5.29 4.33 2.48 10.16 3.06 69.46 7.67 51.85

New Celebration Stage I Mylonite 133565_2-1 Conc. (ppm) 322.59 55.26 50.93 723000.00 17.43 141.24 0.39 117.60 1.08DL 1.25 1.56 1.32 16.14 0.17 0.57 1.81 0.96 1.03Precision(%) 3.15 7.12 3.26 2.50 3.21 3.08 175.72 3.72 39.42

New Celebration Stage I Mylonite 133565_3-1 Conc. (ppm) 300.78 206.64 37.20 723000.00 17.19 122.01 BD BD 1.29DL 0.72 1.26 0.79 13.19 0.12 0.42 1.22 0.78 0.88Precision(%) 4.39 6.34 3.98 3.08 3.44 3.37 29.27

New Celebration Stage I Mylonite 133565_3-2 Conc. (ppm) 645.31 632.24 593.85 723000.00 23.08 138.59 BD 131.69 BDDL 0.51 1.33 0.87 13.89 0.10 0.33 0.95 0.83 1.05Precision(%) 19.33 4.65 25.69 3.02 10.37 3.62 10.44



St Ives 169.45_5-1 Conc. (ppm) 8509.59 2850.82 8553.28 723000.00 332.91 400.36 BD 1685.85 BDDL 33.59 20.85 14.38 401.84 2.61 6.98 18.46 8.73 14.71Precision(%) 8.14 5.53 3.45 3.89 4.82 5.28 5.31

364

Sample No

1250_12-4_1A

1250_12-4_1B

1250_12-4_3-1

1250_12-4_3-2

1250_12-4_3-3

1250_12-4_4-1

1250_12-4_4-2

133565_1-2

133565_2-1

133565_3-1

133565_3-2

133565_4-1

133565_4-2

169.45_5-1

Se82 Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U238

BD 0.11 BD BD BD 1.44 BD BD BD BD BD BD BD BD BD BD BD6.89 0.04 1.09 0.19 5.89 0.25 0.17 2.50 0.15 0.02 0.08 0.07 0.03 0.07 0.03 0.02 0.01

74.96 9.07BD BD BD BD BD 1.29 BD BD BD BD BD BD BD BD BD 0.01 BD

5.99 0.02 1.01 0.21 6.75 0.21 0.16 3.37 0.21 0.02 0.05 0.08 0.03 0.07 0.03 0.01 0.019.27 96.82

BD 90.75 BD BD 7.32 1.04 0.29 BD 0.54 0.06 0.40 BD BD 0.57 BD 0.41 0.287.18 0.04 1.07 0.25 6.44 0.26 0.16 4.54 0.18 0.02 0.06 0.11 0.03 0.07 0.02 0.01 0.01

15.91 33.96 12.48 31.35 30.42 26.14 17.94 13.20 17.47 17.30BD 37.53 BD BD BD 1.43 BD BD BD BD BD BD BD BD BD 0.11 0.10

6.89 0.03 1.21 0.23 6.66 0.26 0.16 4.31 0.17 0.02 0.08 0.09 0.03 0.07 0.03 0.02 0.0121.54 9.21 20.74 23.90

BD 37.70 BD BD BD 0.96 0.09 BD BD BD 0.04 BD BD BD BD 0.12 0.079.70 0.02 1.22 0.22 6.70 0.32 0.09 3.09 0.14 0.01 0.10 0.08 0.03 0.07 0.04 0.02 0.01

13.91 14.19 51.59 145.95 16.27 19.44BD 10.34 BD 0.09 BD 1.28 BD BD BD BD BD BD BD BD BD BD 0.02

8.11 0.04 1.20 0.18 5.94 0.31 0.18 3.26 0.16 0.02 0.09 0.07 0.03 0.07 0.04 0.02 0.0225.62 90.26 10.47 45.61

BD 13.32 BD BD BD 1.04 BD BD BD BD BD BD BD BD BD BD 0.038.87 0.02 1.15 0.24 8.17 0.28 0.20 3.20 0.22 0.02 0.06 0.07 0.02 0.08 0.03 0.02 0.02

23.68 12.77 38.74BD 351.61 BD BD 4.83 1.51 BD BD 2.32 0.03 0.19 BD BD 0.64 BD 2.42 2.35

13.70 0.04 1.30 0.29 6.87 0.41 0.24 2.51 0.40 0.02 0.15 0.10 0.05 0.08 0.06 0.02 0.0219.09 57.10 16.16 80.40 58.26 70.59 23.22 26.69 19.51

BD 69.07 BD BD BD 1.53 BD BD BD 0.02 2.01 BD BD 0.19 BD 0.45 0.4814.27 0.04 1.17 0.27 6.89 0.32 0.20 3.78 0.34 0.02 0.14 0.07 0.04 0.06 0.04 0.02 0.03

15.87 10.59 36.15 15.02 21.13 16.98 13.634.02 BD BD BD BD 0.83 BD 2.36 1.78 0.12 5.28 BD BD 0.68 0.02 0.32 0.277.47 0.02 1.02 0.20 5.71 0.25 0.19 2.33 0.21 0.02 0.11 0.08 0.03 0.06 0.02 0.02 0.01

78.72 14.17 40.56 39.13 28.57 19.05 18.48 48.98 11.79 10.37BD 582.74 BD BD 4.37 1.03 0.65 BD 1.68 5.36 52.22 BD BD 1.81 0.04 3.74 3.29

7.10 0.05 1.11 0.23 4.31 0.26 0.13 3.13 0.17 0.01 0.08 0.08 0.04 0.07 0.03 0.02 0.016.15 39.82 11.94 16.08 14.27 24.50 11.00 6.67 37.85 6.99 6.43

BD 76.20 BD BD BD 0.98 BD BD 0.86 BD 0.84 BD BD 0.17 BD 0.57 0.558.52 0.03 1.01 0.21 5.11 0.26 0.17 3.54 0.15 0.02 0.06 0.09 0.03 0.06 0.02 0.02 0.02

17.02 12.68 19.70 15.94 19.04 15.77 15.63BD 34.02 BD BD BD 5.02 0.17 BD 3.85 0.03 4.72 BD 0.02 0.26 BD 0.26 0.27

7.47 0.06 1.03 0.19 6.13 0.27 0.13 2.85 0.19 0.02 0.10 0.09 0.02 0.06 0.03 0.02 0.0313.19 85.54 37.74 13.76 38.05 18.38 50.80 16.84 16.48 15.60

BD 363.08 BD BD BD 12.70 BD BD 54.11 25.18 1.97 BD 0.57 5.23 0.52 11.26 3.05132.39 0.52 13.63 3.00 92.95 2.78 1.76 43.36 4.16 0.30 1.04 1.42 0.44 0.71 0.37 0.21 0.22

12.66 12.06 18.39 38.70 41.17 42.48 24.33 38.43 33.88 19.17

365

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75St Ives 301.0_1 Conc. (ppm) 763.55 18.50 1015.46 723000.00 28.54 43.92 1.27 43.07 BD

DL 0.82 1.60 0.91 15.43 0.09 0.25 0.89 0.62 3.89Precision(%) 3.61 9.63 7.54 2.57 3.51 3.15 33.80 4.36

St Ives 301.0_2 Conc. (ppm) 68408.80 108.01 10555.88 723000.00 56.94 72.88 3.75 178.60 7.75DL 0.90 2.53 1.06 30.55 0.09 0.49 1.49 0.54 5.19Precision(%) 14.01 7.98 8.62 8.14 7.24 6.56 19.53 8.18 27.06

St Ives 301.0_3 Conc. (ppm) 901.65 6.58 1125.99 723000.00 33.51 44.22 BD 43.29 5.80DL 0.35 1.61 0.93 13.22 0.10 0.35 1.08 0.45 3.58Precision(%) 3.11 12.85 9.84 2.77 3.89 3.19 3.65 23.29

St Ives 42.8_1-2 Conc. (ppm) 152.55 BD 377.41 723000.00 10.91 344.61 7.24 22.80 BDDL 4.03 6.03 3.90 67.81 0.46 1.17 5.23 2.15 5.87Precision(%) 13.29 12.00 11.68 12.65 11.65 45.88 13.75

St Ives 42.8_2-3 Conc. (ppm) 143.82 BD 391.46 723000.00 12.20 278.27 BD 23.40 BDDL 3.21 5.23 3.79 52.96 0.44 1.16 5.64 2.29 4.75Precision(%) 13.48 10.74 10.60 11.71 10.48 12.49

St Ives 42.8_2-4 Conc. (ppm) 157.64 BD 1048.04 723000.00 51.38 425.47 153.65 586.34 BDDL 2.81 3.52 3.01 48.33 0.40 1.00 4.09 2.34 3.36Precision(%) 10.25 9.93 5.93 21.84 7.49 30.66 19.38




Golden Mile Chron. Samples Fimiston Stage II 52280_1-3 Conc. (ppm) 2581673.92 BD 4959.45 723000.00 BD BD 46.85 497.77 2364.64DL 8.93 11.98 8.35 157.23 0.70 3.36 11.00 5.98 13.34Precision(%) 7.57 6.43 7.66 12.76 14.02 9.57

Golden Mile Chron. Samples Fimiston Stage II 52280_2-2 Conc. (ppm) 922848.25 BD 12440.41 723000.00 BD BD BD 976.57 559.87DL 36.96 17.45 13.59 200.62 1.05 3.67 17.28 10.18 23.18Precision(%) 6.40 6.49 5.79 7.02 6.51

Golden Mile Chron. Samples Fimiston Stage II 52280_2-4 Conc. (ppm) 212771.67 BD 3334.23 723000.00 131.14 15.86 38.71 246.35 860.62DL 13.01 5.93 4.78 70.91 0.48 2.02 6.24 4.15 7.51Precision(%) 15.12 11.40 8.31 12.58 13.18 13.03 11.16 11.75

Golden Mile Fimiston Aberdare ABD15_5 Conc. (ppm) 14620.65 7.67 31.17 723000.00 6184.36 5390.29 229.82 43.44 10371.52DL 6.58 1.55 1.02 15.97 0.11 0.41 1.30 0.80 4.36Precision(%) 11.74 21.68 13.07 5.51 5.59 9.74 10.00 12.10 7.51

Golden Mile Fimiston Aberdare ABD15_6 Conc. (ppm) 926466.21 134.59 978.74 723000.00 6358.36 3011.71 1094.72 198.24 13414.71DL 12.22 4.52 1.77 33.81 0.32 0.80 3.75 1.67 11.19Precision(%) 7.31 8.31 8.71 6.89 8.49 8.18 15.88 8.41 7.14

Golden Mile Fimiston Aberdare ABD9_1 Conc. (ppm) 63.53 1.90 169.23 723000.00 47.52 66.02 BD 103.79 6.42

366

Sample No301.0_1

301.0_2

301.0_3

42.8_1-2

42.8_2-3

42.8_2-4

43.1_2-1

43.1_2-2

43.1_2-3

52280_1-3

52280_2-2

52280_2-4

ABD15_5

ABD15_6

ABD9_1

Se82 Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U238BD 7.91 BD BD BD 1.61 BD BD 8.74 5.11 0.12 BD BD 1.39 BD 0.04 0.06

13.50 0.03 1.24 0.18 5.77 0.26 0.14 2.71 0.15 0.02 0.09 0.10 0.03 0.06 0.03 0.02 0.0268.10 10.66 9.83 8.54 37.72 9.67 21.98 29.51

11.43 278.76 BD BD BD 7.49 1.48 BD 233.52 173.20 5.69 BD 0.09 9.31 0.03 11.57 6.0013.12 0.05 1.49 0.23 7.09 0.40 0.23 3.45 0.23 0.02 0.11 0.17 0.06 0.06 0.01 0.03 0.0246.23 30.27 8.73 17.52 12.50 10.26 12.73 28.67 10.14 34.04 21.75 17.27

BD 2.87 BD BD BD 1.65 BD BD 9.36 8.99 0.13 BD 0.03 0.49 BD 0.07 0.0311.16 0.04 1.45 0.20 6.45 0.30 0.12 3.18 0.16 0.02 0.08 0.08 0.02 0.06 0.02 0.02 0.02

18.37 9.37 9.61 12.06 33.48 39.11 13.35 17.17 28.09BD BD BD BD BD 2.01 BD BD BD BD BD BD BD BD 0.40 0.03 BD

36.72 0.10 4.38 0.92 21.17 1.19 0.67 11.91 0.91 0.08 0.27 0.18 0.13 0.23 0.27 0.03 0.0726.55 63.75 55.82

BD BD BD BD BD 1.66 BD BD 1.10 0.06 BD BD BD BD BD BD 0.0237.06 0.15 4.52 0.61 21.80 1.10 0.42 10.81 0.66 0.04 0.33 0.17 0.12 0.23 0.11 0.06 0.02

28.45 39.52 43.43 58.542.98 BD BD BD BD 1.50 0.88 BD 3.44 BD 5.28 BD BD 0.40 0.99 BD BD

35.28 0.07 4.11 0.43 17.39 0.73 0.41 9.45 0.42 0.06 0.18 0.30 0.09 0.13 0.04 0.05 0.02442.37 21.00 28.45 16.77 25.31 22.58 19.68

BD 0.73 BD BD BD BD BD BD BD BD BD BD BD BD BD BD BD75.30 0.36 8.79 2.25 47.83 2.96 1.63 22.74 2.37 0.11 0.87 0.64 0.35 0.65 0.20 0.12 0.22

54.36BD 16.18 BD BD BD 3.80 BD BD 8.36 BD BD BD BD BD BD BD BD

234.89 0.58 36.41 6.74 160.05 10.56 4.93 86.35 4.66 0.93 2.72 2.28 0.98 2.36 0.80 0.43 0.3221.57 106.77 33.93

BD 30.47 4.83 BD BD 11.74 14.97 BD 9.15 7.10 BD BD BD 3.25 3.05 0.83 BD304.28 1.08 49.03 8.84 228.70 10.62 4.93 106.16 5.55 0.57 3.58 2.92 0.81 1.97 1.10 0.37 0.61

19.70 383.40 41.37 26.36 35.12 31.56 36.96 28.67 39.27BD 1731.05 BD BD BD 475.42 9410.35 BD 464.18 192.14 24453.77 BD 0.27 59.99 BD 27.30 42.95

58.48 0.20 9.48 1.61 47.24 2.53 1.70 16.35 1.79 0.12 0.62 0.77 0.23 0.44 0.16 0.09 0.1115.34 8.64 9.58 8.30 8.10 8.58 40.74 8.78 8.04 8.90

BD 1532.61 184.66 BD BD 179.88 2630.28 BD 326.31 38.85 7191.57 BD 1.29 70.95 BD 3.60 7.8675.58 0.42 12.10 2.49 61.04 3.06 2.01 28.11 1.83 0.26 0.51 0.76 0.25 0.81 0.27 0.18 0.17

14.05 13.04 7.60 5.67 11.98 11.56 8.83 16.77 8.56 10.59 9.26BD 262.45 BD BD BD 48.98 490.59 BD 419.88 9.34 1661.69 2.37 1.75 47.25 1.90 0.99 1.95

40.96 0.11 4.64 0.95 26.66 1.37 0.45 13.45 0.86 0.07 0.39 0.32 0.11 0.18 0.11 0.07 0.0527.65 15.87 15.35 15.61 19.80 18.54 16.91 13.40 7.93 13.70 20.80 21.98

23.70 10.72 BD 4.37 BD 2.97 204.27 12.23 65.47 0.62 44.36 2.38 21.31 93.30 3.16 0.05 0.1210.23 0.04 1.62 0.29 7.95 0.34 0.21 3.77 0.25 0.03 0.12 0.15 0.03 0.07 0.05 0.04 0.0222.24 13.45 8.76 9.61 11.56 17.23 16.60 12.83 11.82 9.93 7.50 5.18 6.07 36.08 20.7446.22 2691.55 3.83 4.03 BD 89.28 2388.52 BD 105.23 64.54 3606.01 0.96 12.29 162.95 2.17 21.32 14.0932.81 0.09 2.45 0.56 12.96 0.85 0.43 8.00 0.41 0.05 0.25 0.22 0.11 0.14 0.06 0.06 0.0427.00 12.87 28.41 12.13 12.04 6.56 7.92 8.58 7.29 16.66 9.66 5.43 8.39 7.01 7.44

BD 1.68 BD BD BD 0.67 0.55 BD BD BD BD BD BD 0.14 BD 0.01 0.02

367

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75DL 0.67 1.23 0.87 12.08 0.08 0.59 0.95 0.46 3.25Precision(%) 5.00 31.19 25.86 2.31 2.64 2.67 5.44 20.33

Golden Mile Fimiston Aberdare ABD9_2 Conc. (ppm) 90.44 4.72 6.54 723000.00 37.06 118.80 BD 74.05 5.72DL 0.55 1.41 0.64 11.36 0.09 0.38 0.87 0.53 2.72Precision(%) 3.61 16.41 10.72 2.53 2.82 3.00 4.60 19.72



Golden Mile Fimiston Aberdare ADGD1/12_1-3 Conc. (ppm) 298.02 1.60 145.13 723000.00 368.53 149.67 26.23 157.82 549.96DL 0.81 0.96 0.80 10.85 0.09 0.29 1.02 0.54 4.01Precision(%) 17.00 29.07 20.37 3.79 15.49 13.09 16.61 5.42 13.64

Golden Mile Fimiston Aberdare ADGD1/12_1-4 Conc. (ppm) 71.86 BD 5.77 723000.00 0.55 15.22 BD 234.38 13.20DL 0.62 1.22 0.74 24.24 0.09 0.35 1.11 0.52 5.15Precision(%) 5.61 14.44 2.24 12.12 4.32 8.18 20.10

Golden Mile Fimiston Depth D12_2-1 Conc. (ppm) 73.98 5.50 35.70 723000.00 1.85 259.25 1.93 44.06 27.06DL 0.81 1.70 1.23 16.62 0.10 0.31 1.85 1.33 8.70Precision(%) 3.89 17.70 16.47 2.62 9.61 2.83 42.16 4.18 15.14

Golden Mile Fimiston Depth D12_2-2 Conc. (ppm) 64.61 8.80 5.30 723000.00 0.76 182.96 BD 33.29 14.29DL 1.16 1.81 1.36 17.24 0.12 0.42 1.56 0.99 11.87Precision(%) 5.89 15.95 12.21 2.18 18.59 2.82 407.80 6.88 34.57

Golden Mile Eastern Lode Great Boulder Main GBM77_1-1 Conc. (ppm) 102.34 0.35 47.79 723000.00 0.53 16.58 BD 41.82 10.42DL 0.71 1.77 0.98 12.47 0.08 0.30 0.86 0.73 8.86Precision(%) 4.22 192.09 8.75 2.44 10.55 4.43 6.48 42.73

Golden Mile Eastern Lode Great Boulder Main GBM77_1-2 Conc. (ppm) 142.84 BD 332.31 723000.00 0.36 10.53 BD 42.39 22.42DL 0.64 1.52 1.09 13.12 0.09 0.21 0.98 0.70 11.00Precision(%) 8.33 7.58 2.27 13.63 5.02 8.69 25.68

Golden Mile Eastern Lode Great Boulder Main GBM77_2 Conc. (ppm) 147.33 BD 150.33 723000.00 0.82 17.25 BD 43.03 4.95DL 0.76 1.41 0.95 14.07 0.10 0.41 1.09 0.30 9.13Precision(%) 6.22 11.98 2.34 8.70 4.21 6.11 71.48



Golden Mile Western Lode Lake View LV27_4 Conc. (ppm) 168400.77 4.38 891.52 723000.00 1643.23 541.08 210.57 387.54 1000.25DL 3.93 6.20 4.08 68.31 0.38 1.19 5.83 2.86 35.87Precision(%) 14.29 57.16 14.55 10.25 10.99 10.19 11.82 9.57 10.70

Golden Mile Western Lode Lake View LV27_4-2 Conc. (ppm) 192204.91 1.34 4.69 723000.00 215.03 86.37 38.42 19.10 461.94DL 12.81 1.80 1.53 45.67 0.15 0.56 1.98 0.98 12.80

368

Sample No

ABD9_2

ABD9_3

ABD9_4

ADGD1/12_1-3

ADGD1/12_1-4

D12_2-1

D12_2-2

GBM77_1-1

GBM77_1-2

GBM77_2

GBM77_3-1

GBM77_3-2

LV27_4

LV27_4-2

Se82 Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U23810.76 0.02 1.02 0.17 5.22 0.23 0.11 2.75 0.16 0.02 0.06 0.07 0.03 0.05 0.02 0.01 0.01

25.71 16.06 14.57 26.11 63.37 25.72BD 0.93 BD BD BD 0.82 0.39 BD 0.19 BD BD BD BD BD BD BD BD

7.86 0.03 0.94 0.20 4.87 0.24 0.19 3.07 0.14 0.02 0.07 0.06 0.02 0.06 0.01 0.02 0.0121.11 13.03 23.26 38.51

BD 4.47 BD BD 1.11 0.84 BD BD 0.07 0.34 BD BD 0.14 BD BD BD9.48 0.04 1.19 0.15 4.96 0.22 0.14 2.90 0.17 0.01 0.05 0.07 0.03 0.04 0.02 0.01 0.01

25.46 9.64 12.16 15.93 14.40 29.75BD 10.50 BD BD BD 1.29 2.25 BD 0.65 0.40 0.32 BD 0.03 2.96 BD 0.01 0.05

9.82 0.03 1.35 0.15 6.83 0.26 0.15 3.30 0.20 0.02 0.08 0.06 0.03 0.05 0.03 0.01 0.0224.94 10.44 12.61 22.21 14.04 36.34 38.18 66.11 51.70 22.12

17.09 86.65 BD 0.66 BD 1.34 12.80 BD 17.19 0.07 1.88 BD 0.03 31.50 0.89 0.06 BD10.23 0.04 1.21 0.20 4.66 0.21 0.11 2.64 0.12 0.02 0.09 0.08 0.03 0.06 0.03 0.01 0.0226.95 25.94 21.16 9.05 11.29 20.77 16.50 10.75 45.11 13.32 14.36 21.45

6.97 0.31 BD BD BD 1.23 0.82 BD 0.28 BD 0.55 BD BD BD BD BD BD10.86 0.05 1.38 0.15 5.61 0.25 0.15 3.78 0.13 0.02 0.04 0.11 0.03 0.06 0.03 0.02 0.0160.94 14.17 10.61 19.31 38.50 22.06

BD 5.07 BD BD BD 2.75 0.21 BD BD BD 0.45 BD BD 0.28 0.02 BD BD10.93 0.04 1.32 0.27 6.05 0.31 0.19 2.97 0.18 0.03 0.10 0.09 0.03 0.07 0.02 0.02 0.02

17.49 6.61 43.11 64.95 17.61 62.64BD 12.48 BD BD BD 2.86 BD BD BD 0.03 0.11 BD BD 0.41 BD 0.12 0.02

12.30 0.04 0.97 0.17 6.21 0.32 0.19 2.94 0.22 0.02 0.09 0.09 0.04 0.07 0.02 0.02 0.0222.90 8.28 47.95 49.04 26.42 51.80 54.18

BD 0.12 0.98 BD BD 1.01 0.19 BD BD 0.03 0.03 BD BD 0.23 BD BD BD9.22 0.03 0.92 0.20 6.43 0.27 0.11 3.43 0.23 0.01 0.08 0.12 0.03 0.06 0.03 0.01 0.01

48.86 40.60 12.05 31.65 28.95 116.65 73.93BD BD BD BD BD 1.02 0.46 BD BD 0.09 0.09 BD BD 0.05 BD BD BD

8.76 0.05 1.47 0.18 6.43 0.31 0.16 3.19 0.20 0.02 0.08 0.12 0.04 0.05 0.03 0.02 0.0212.58 19.37 45.76 57.02 46.08

BD BD BD BD BD 0.97 BD BD BD 0.02 0.07 0.07 BD BD BD 1.24 BD9.55 0.04 1.14 0.13 5.70 0.26 0.19 3.17 0.14 0.02 0.07 0.05 0.03 0.06 0.03 0.02 0.02

13.05 61.22 52.68 38.36 100.99BD 0.24 BD BD BD 1.92 3.47 BD 0.30 0.03 0.22 BD 0.05 0.06 BD BD 0.03

10.99 0.04 1.19 0.20 5.57 0.19 0.14 2.87 0.14 0.02 0.06 0.09 0.04 0.08 0.03 0.02 0.0236.58 6.92 10.74 29.76 27.97 21.19 35.54 49.67 27.98

BD 6.06 BD BD BD 1.39 0.40 BD 0.19 0.02 0.07 0.03 BD BD BD BD BD8.79 0.02 1.32 0.17 5.59 0.36 0.14 3.26 0.19 0.02 0.10 0.11 0.03 0.07 0.03 0.02 0.02

17.31 11.60 19.46 45.54 48.62 60.20 133.84BD 18.48 BD 1.53 BD 16.17 197.61 BD 375.84 6.81 506.95 3.59 1.39 39.26 4.29 0.75 0.55

35.50 0.16 4.39 0.85 21.37 1.31 0.43 12.00 0.90 0.09 0.40 0.29 0.14 0.22 0.11 0.06 0.0612.93 30.77 9.78 13.38 11.57 16.06 13.75 14.77 12.55 9.96 11.92 18.63 18.30

BD 48.07 BD BD BD 9.57 195.86 3.10 14.40 7.65 511.96 0.35 0.48 10.96 0.81 0.95 0.5914.04 0.06 1.57 0.26 8.71 0.41 0.27 3.67 0.25 0.02 0.17 0.11 0.05 0.08 0.03 0.01 0.02

369

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75Precision(%) 3.98 54.26 13.71 3.78 6.68 6.14 7.56 6.24 4.35

Golden Mile Western Lode Lake View LV27_5 Conc. (ppm) 44900.59 22.50 297.69 723000.00 35.13 43.67 5.37 78.10 67.97DL 1.10 1.43 1.38 17.40 0.11 0.52 1.85 0.72 11.10Precision(%) 20.38 13.58 16.67 3.41 16.63 6.92 20.93 6.96 11.52

Golden Mile Western Lode Lake View LV37_1-3 Conc. (ppm) 228809.76 9.16 45.51 723000.00 1079.47 340.69 916.13 30.14 8634.13DL 1.12 1.38 1.23 18.83 0.11 0.34 1.66 0.72 7.85Precision(%) 3.05 10.31 5.28 3.00 3.03 3.71 5.39 4.87 3.46

Golden Mile Western Lode Lake View LV37_1-4 Conc. (ppm) 217994.25 5.08 11.31 723000.00 1994.55 384.11 458.58 32.58 6076.92DL 1.16 1.24 1.00 18.08 0.10 0.33 1.24 0.75 7.99Precision(%) 3.32 13.31 11.38 2.52 2.89 3.57 3.95 4.06 3.91

Golden Mile Western Lode Lake View LV53_1-1 Conc. (ppm) 165.79 BD 8.66 723000.00 1.04 24.70 BD 26.97 9.46DL 1.12 2.14 1.41 56.19 0.15 0.55 1.67 1.13 6.70Precision(%) 4.92 7.15 2.56 9.40 4.33 6.27 29.79

Golden Mile Western Lode Lake View LV53_2-1 Conc. (ppm) 375.78 8.10 9.27 723000.00 0.35 30.95 BD 50.62 13.55DL 1.20 1.84 1.28 18.56 0.15 0.37 1.44 0.83 7.31Precision(%) 12.76 14.59 8.09 2.58 18.95 3.97 5.98 22.04

Golden Mile Western Lode Lake View LV53_2-2 Conc. (ppm) 94.20 BD 7.60 723000.00 8.11 26.73 BD 12.02 BDDL 1.12 2.23 1.42 24.74 0.12 0.38 1.81 1.11 7.76Precision(%) 5.37 8.36 2.58 3.51 4.05 7.37

370

Sample No

LV27_5

LV37_1-3

LV37_1-4

LV53_1-1

LV53_2-1

LV53_2-2

Se82 Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2388.50 4.53 3.62 50.52 6.64 4.88 4.08 19.17 8.83 4.82 7.03 5.46 5.73

BD 23.33 BD BD BD 2.86 31.02 BD 1.68 0.83 96.02 BD 0.04 2.48 0.09 0.11 0.0413.84 0.04 1.76 0.25 6.19 0.33 0.21 3.47 0.30 0.01 0.06 0.14 0.04 0.06 0.02 0.02 0.01

11.64 13.69 18.60 18.40 9.27 18.24 41.62 13.67 26.33 19.10 30.8431.11 434.39 7.84 24.59 BD 9.00 459.01 352.43 10.77 3.80 2566.46 65.34 5.08 154.68 0.91 0.33 0.5210.17 0.04 1.09 0.19 5.91 0.38 0.16 2.94 0.14 0.02 0.09 0.08 0.03 0.04 0.02 0.02 0.0114.96 11.80 18.16 3.85 4.12 2.78 4.69 6.71 3.77 3.29 5.76 3.66 2.99 5.84 8.05 5.7127.05 576.04 10.93 27.53 6.46 9.14 430.14 398.06 12.05 2.87 2175.20 42.52 5.73 167.93 1.08 0.52 0.718.16 0.05 1.10 0.20 5.52 0.43 0.24 3.99 0.08 0.03 0.08 0.09 0.04 0.09 0.02 0.01 0.02

14.07 11.82 41.74 3.56 33.21 4.30 3.67 4.60 5.95 3.96 2.83 5.68 4.48 3.06 5.05 5.26 5.01BD 0.37 BD BD BD 1.55 BD BD BD BD BD BD BD BD BD BD BD

9.28 0.04 1.29 0.25 5.54 0.38 0.16 3.34 0.27 0.02 0.11 0.12 0.04 0.08 0.04 0.02 0.0230.13 11.17

BD 33.66 BD BD BD 1.43 0.52 BD BD 0.07 12.91 BD BD BD BD BD 0.0212.37 0.05 1.61 0.27 7.70 0.36 0.13 3.20 0.23 0.02 0.14 0.11 0.03 0.07 0.03 0.03 0.01

15.08 12.10 18.75 21.12 11.30 42.1510.85 4.21 BD BD BD 1.37 BD BD BD 0.01 BD 0.04 BD BD 0.02 0.01 BD10.78 0.17 1.49 0.27 7.04 0.39 0.17 3.36 0.24 0.01 0.08 0.00 0.03 0.08 0.02 0.01 0.0240.79 36.14 13.35 81.34 40.35 50.17 78.99

371

Location Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82 Zr90 Mo95 Ag107 Cd111

New Celebration JD0475-5_1-1 Conc. (ppm) 415845.42 11.26 15319.37 500000.00 71.16 52.31 6.18 349.19 6.13 BD 8.11 1.62 BD BDDL 1.27 2.64 1.39 18.08 0.20 0.69 1.68 0.88 1.45 10.62 0.06 1.62 0.30 10.77Precision(%) 3.22 12.03 3.02 3.08 3.18 5.17 14.01 2.89 12.73 16.84 39.17

New Celebration JD0475-5_2-1 Conc. (ppm) 392601.58 15.19 14049.28 500000.00 106.41 133.53 10.24 382.30 4.99 BD 108.68 11.32 BD BDDL 6.85 1.65 1.52 23.31 0.20 0.64 1.39 1.36 1.63 12.50 0.04 1.70 0.41 9.21Precision(%) 4.27 10.21 3.74 3.18 3.69 12.29 14.80 3.60 16.15 19.31 48.36

New Celebration JD0475-5_2-2 Conc. (ppm) 411517.79 7.88 16516.40 500000.00 67.72 33.28 4.62 331.03 2.30 BD 5.89 BD BD BDDL 4.34 1.70 1.32 21.26 0.15 0.39 1.35 1.11 1.44 8.53 0.06 1.49 0.29 7.35Precision(%) 3.24 11.79 3.17 3.12 3.26 4.47 14.04 3.18 28.09 7.39

New Celebration JD0475-5_4-1 Conc. (ppm) 398055.50 7.97 14820.39 500000.00 46.03 335.30 8.98 384.39 4.88 BD 40.97 BD BD 9.29DL 11.89 2.48 1.39 23.99 0.17 0.47 1.84 0.91 0.97 11.91 0.05 1.46 0.35 8.66Precision(%) 3.30 15.30 3.23 3.20 3.38 4.75 31.51 2.89 12.12 13.36 38.18

New Celebration JD0475-5_4-2 Conc. (ppm) 393920.52 16.64 14446.52 500000.00 50.62 510.43 6.27 368.28 4.83 BD 8.13 BD BD BDDL 1.66 1.94 1.65 21.10 0.22 0.67 1.31 0.90 1.29 13.08 0.05 1.59 0.31 10.96Precision(%) 4.34 9.91 3.99 3.49 5.01 11.13 13.92 3.79 14.81 10.41

St Ives 169.45_4-1 Conc. (ppm) 430030.98 388.00 30086.19 500000.00 89.98 48.28 BD 261.43 BD BD 236.48 BD BD BDDL 44.90 6.95 4.97 82.11 0.55 1.49 4.51 2.71 3.55 38.13 0.28 3.89 0.77 17.45Precision(%) 7.15 13.40 6.22 5.24 5.52 14.41 9.77 12.93

St Ives 169.45_5-2 Conc. (ppm) 488056.32 209.29 31138.44 500000.00 98.62 32.65 BD 382.73 3.80 BD 106.81 4.42 BD BDDL 19.63 5.97 4.05 83.77 0.48 1.87 5.04 2.43 3.69 45.62 0.19 4.47 0.89 26.49Precision(%) 4.13 6.88 3.95 4.24 7.73 8.47 19.94 19.96 40.61

St Ives 317.15_2-1 Conc. (ppm) 286181.82 2442.11 23692.25 500000.00 145.01 194.71 BD 569.52 BD BD 103.74 BD BD BDDL 149.03 77.96 78.64 951.30 8.22 25.70 71.25 48.74 62.96 642.56 2.80 73.87 12.29 322.30Precision(%) 14.01 14.50 12.84 13.03 15.47 19.16 16.77 13.31

372

Sample No

JD0475-5_1-1

JD0475-5_2-1

JD0475-5_2-2

JD0475-5_4-1

JD0475-5_4-2

169.45_4-1

169.45_5-2

317.15_2-1

Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U238

6.85 5.57 BD 0.88 0.09 16.52 BD BD 0.74 0.07 0.04 0.070.43 0.23 6.69 0.23 0.04 0.15 0.11 0.05 0.08 0.04 0.02 0.025.33 5.99 22.33 34.72 4.49 10.28 28.66 39.24 22.067.25 5.13 BD 0.90 0.15 17.84 BD BD 1.10 0.05 0.05 0.150.40 0.26 5.98 0.31 0.03 0.14 0.14 0.05 0.09 0.04 0.02 0.027.38 6.74 18.30 21.12 5.34 7.67 38.50 25.19 13.765.57 4.53 BD 1.05 0.15 17.66 BD BD 2.19 0.06 0.02 0.190.35 0.14 4.28 0.28 0.03 0.13 0.11 0.04 0.07 0.03 0.02 0.025.29 6.15 15.79 13.67 3.71 7.72 28.20 37.30 9.45

15.95 5.11 BD 0.41 BD 17.37 0.04 BD 0.63 0.04 BD 0.050.44 0.23 5.24 0.30 0.02 0.12 0.11 0.06 0.09 0.03 0.02 0.02

60.87 6.02 34.23 3.95 144.16 9.60 35.56 19.0067.34 3.82 BD 16.11 0.03 12.33 BD 0.04 1.42 0.09 0.06 0.070.42 0.17 5.03 0.16 0.03 0.12 0.09 0.04 0.09 0.03 0.02 0.02

56.66 6.62 13.36 51.20 4.48 48.81 9.97 71.04 18.45 22.934.56 1.11 BD 3.70 0.31 10.54 BD BD 1.20 BD 0.74 0.700.96 0.75 11.89 0.61 0.09 0.41 0.21 0.11 0.21 0.09 0.07 0.06

10.73 31.87 16.75 20.05 9.43 15.30 12.47 12.636.00 3.02 BD 1.83 0.79 13.04 0.24 BD 1.72 0.58 0.44 0.701.35 0.60 14.00 0.75 0.11 0.35 0.16 0.12 0.20 0.06 0.09 0.06

10.43 12.68 26.68 14.53 6.45 39.65 25.36 15.75 19.10 16.3298.43 212.79 BD 14.54 30.04 BD BD BD 112.22 2.53 27.77 13.4717.81 10.86 235.06 9.45 1.26 58.69 4.49 1.96 3.69 1.17 1.14 1.0617.35 17.92 38.81 13.87 15.28 28.60 13.76 17.56

373

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82

St Ives 169.45_1-1 Conc. (ppm) 4.55 BD BD 635000.00 1469.16 2749.51 BD BD BD 49.38DL 0.93 1.00 0.87 24.25 0.26 0.38 0.83 0.83 0.95 7.45Precision(%) 12.28 2.90 3.01 2.94 8.41

St Ives 169.45_1-2 Conc. (ppm) 5.19 BD BD 635000.00 1555.30 2799.00 BD 0.91 BD 38.44DL 0.87 1.16 0.83 49.35 0.32 0.77 1.11 0.68 0.85 7.51Precision(%) 10.58 2.80 3.01 2.89 32.77 9.28

St Ives 169.45_2-1 Conc. (ppm) 5.77 BD 45.34 635000.00 1618.21 2966.59 BD 1.52 BD 44.08DL 0.49 1.09 0.96 17.20 0.18 0.52 0.79 0.50 0.75 7.85Precision(%) 9.09 45.35 2.87 3.61 2.99 18.40 8.37

St Ives 169.45_3-1 Conc. (ppm) 5.08 BD 3.23 635000.00 1471.47 2794.70 BD 0.83 BD 42.23DL 0.60 0.90 0.77 11.18 0.08 0.40 0.71 0.48 0.73 7.89Precision(%) 9.43 27.12 2.78 2.92 2.90 27.83 9.23

St Ives 169.45_3-3 Conc. (ppm) 4.80 BD BD 635000.00 1532.08 2815.76 BD 0.66 BD 42.30DL 0.87 1.17 0.76 46.25 0.54 0.27 1.00 0.65 0.87 7.86Precision(%) 11.40 2.87 2.94 2.89 44.66 9.08

St Ives 213.1_1 Conc. (ppm) 11.65 5.71 17.46 635000.00 1049.34 1157.16 357.54 1.81 4.75 57.45DL 0.32 0.97 0.79 10.31 0.06 0.27 1.00 0.37 4.06 7.01Precision(%) 6.29 13.09 5.06 2.99 3.32 3.15 23.26 15.30 33.35 6.75



St Ives 213.3_4 Conc. (ppm) 12.36 1.45 10.58 635000.00 935.89 1083.21 BD 1.64 6.31 58.07DL 0.95 1.18 0.75 15.71 0.07 0.14 0.76 0.62 3.88 5.51Precision(%) 8.92 38.52 9.92 2.61 3.11 2.54 19.06 24.83 5.78

St Ives 323.0_1 Conc. (ppm) 23.24 BD 11.84 635000.00 1056.66 4.90 BD 1.02 2.96 23.92DL 0.52 0.84 0.57 10.62 0.09 0.15 0.68 0.42 2.82 6.65Precision(%) 26.95 13.68 2.74 2.85 6.01 23.32 37.73 12.78

St Ives 323.0_2 Conc. (ppm) 184.75 BD 127.03 635000.00 959.00 7.44 24936.63 45.60 3.64 18.05DL 0.70 1.38 0.82 33.34 0.09 0.26 0.80 0.76 3.30 9.39Precision(%) 11.68 9.69 5.72 5.99 16.40 11.11 14.24 36.46 22.29

St Ives 323.0_3 Conc. (ppm) 57.35 BD 64.64 635000.00 1017.18 5.31 BD 5.86 BD 23.87DL 0.55 1.31 0.61 15.16 0.11 0.24 0.82 0.43 2.81 6.47Precision(%) 10.71 13.46 3.47 3.62 11.46 18.38 12.43

St Ives 323.0_4 Conc. (ppm) 834.59 BD 1062.29 635000.00 908.33 5.14 1.32 112.79 6.87 24.47DL 1.40 2.63 1.25 39.94 0.14 0.48 1.52 0.74 4.86 15.22Precision(%) 11.04 10.74 12.33 13.94 14.84 48.46 11.16 29.25 26.76

St Ives 423.0_1-3 Conc. (ppm) 95.65 1.89 1972.18 635000.00 204.01 669.40 BD 3.25 BD 29.11

374

Sample No

169.45_1-1

169.45_1-2

169.45_2-1

169.45_3-1

169.45_3-3

213.1_1

213.1_2

213.3_2

213.3_4

323.0_1

323.0_2

323.0_3

323.0_4

423.0_1-3

Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U238

BD BD BD BD 1.43 BD BD BD BD BD BD BD 0.59 0.17 BD BD0.03 0.98 0.19 4.82 0.23 0.15 2.28 0.18 0.02 0.05 0.05 0.02 0.05 0.01 0.01 0.01

8.51 7.79 10.16BD BD 0.73 BD 1.06 BD BD BD BD BD BD 0.19 2.74 0.67 0.01 BD

0.04 0.94 0.17 4.85 0.26 0.12 2.40 0.15 0.01 0.05 0.07 0.02 0.05 0.02 0.01 0.0114.62 10.92 15.79 8.33 10.07 99.46

BD BD 0.41 BD 1.26 BD 7.78 0.18 BD BD BD 0.18 10.36 0.80 BD BD0.04 0.94 0.16 4.61 0.23 0.16 2.12 0.10 0.02 0.05 0.08 0.03 0.04 0.02 0.01 0.01

34.11 8.90 50.21 34.72 14.26 43.48 27.96BD BD 0.53 BD 1.13 BD 0.59 BD BD BD BD BD 2.07 0.51 BD BD

0.03 0.80 0.16 3.98 0.19 0.16 2.88 0.14 0.02 0.08 0.08 0.03 0.05 0.03 0.01 0.0116.67 8.61 187.35 7.25 6.63

BD BD BD BD 1.30 BD BD BD BD BD BD 0.02 0.31 0.10 BD BD0.00 0.79 0.20 4.50 0.21 0.14 2.17 0.14 0.02 0.06 0.04 0.02 0.05 0.02 0.01 0.00

7.95 42.72 12.14 14.050.04 BD 1.02 BD 1.02 BD BD BD 0.44 0.12 BD 0.03 7.25 2.04 0.01 0.060.03 1.09 0.16 4.50 0.28 0.18 2.61 0.15 0.02 0.06 0.07 0.02 0.07 0.02 0.01 0.01

39.43 14.71 12.50 11.37 30.66 37.64 4.37 10.37 75.97 14.7726.18 BD 1.01 BD 2.12 1.20 3.62 89.65 14.88 1.65 BD 0.07 5.67 1.47 0.63 1.110.02 1.51 0.25 8.12 0.31 0.19 3.10 0.22 0.02 0.12 0.07 0.04 0.06 0.02 0.03 0.02

21.56 17.19 11.01 14.73 17.89 10.70 13.72 24.98 8.57 9.42 12.19 10.831.11 BD 2.99 BD 1.01 0.34 BD 0.23 0.03 BD BD 0.10 11.78 1.79 BD 0.010.04 0.97 0.15 4.57 0.26 0.11 3.18 0.16 0.01 0.07 0.09 0.02 0.06 0.02 0.02 0.019.21 13.51 11.98 16.87 31.87 28.51 13.90 3.68 5.88 55.94

12.20 BD 2.01 BD 1.00 BD 2.94 1.65 0.06 BD BD 0.06 2.34 2.44 BD 0.080.03 1.01 0.17 4.63 0.24 0.14 2.44 0.15 0.02 0.08 0.07 0.02 0.04 0.02 0.02 0.02

52.09 36.84 11.78 47.85 21.82 21.52 18.83 6.01 32.31 56.951.57 BD BD BD 0.87 BD BD BD 0.98 BD BD BD 3.59 0.52 0.16 0.110.03 0.97 0.19 4.14 0.22 0.12 2.07 0.15 0.01 0.05 0.05 0.02 0.05 0.02 0.01 0.01

15.95 10.88 14.55 19.31 9.38 15.13 15.9543.64 BD 4.04 BD 1.33 0.25 BD 25.74 21.11 0.30 BD 0.23 14.58 5.15 1.05 2.310.03 1.04 0.16 4.14 0.24 0.13 2.57 0.15 0.02 0.06 0.07 0.02 0.05 0.01 0.01 0.01

36.51 11.13 10.56 27.01 10.82 14.51 19.48 11.02 9.05 9.35 16.46 11.5673.83 BD 0.44 BD 1.08 BD BD 6.29 16.86 0.18 0.00 0.09 32.49 5.47 2.32 2.050.05 0.98 0.16 4.53 0.22 0.13 2.29 0.18 0.01 0.06 0.08 0.02 0.04 0.02 0.01 0.01

19.25 22.24 10.20 11.43 11.45 21.66 887.37 16.75 43.44 13.00 14.17 10.6110.77 BD BD BD 2.35 0.35 BD 23.21 19.13 BD BD BD 8.38 0.86 2.35 1.550.03 1.28 0.24 8.96 0.34 0.14 3.01 0.26 0.03 0.11 0.11 0.05 0.10 0.04 0.02 0.02

18.42 210.40 11.69 28.30 12.40 15.51 36.78 15.88 18.13 14.791.82 BD 7.37 BD 0.79 0.61 5.94 15.52 0.05 0.12 BD 0.04 11.57 1.52 0.04 BD

375

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82DL 0.74 1.29 0.74 13.33 0.25 0.25 1.16 0.61 2.72 7.10Precision(%) 25.13 39.77 14.19 3.35 3.45 3.43 19.65 10.84

St Ives 423.0_1-4 Conc. (ppm) 1381.03 25.31 226.70 635000.00 231.13 722.24 BD 21.06 BD 51.94DL 2.98 5.40 3.12 55.74 0.50 1.05 3.57 2.84 14.72 30.61Precision(%) 27.02 26.06 18.31 24.27 26.06 24.39 20.44 30.04

St Ives 423.0_2-1 Conc. (ppm) 6.28 BD 1.91 635000.00 160.72 559.40 BD 1.42 3.26 25.17DL 0.42 0.75 0.49 11.57 0.06 0.25 0.65 0.22 1.86 4.77Precision(%) 7.97 33.21 3.25 3.43 3.30 12.93 24.52 9.51

St Ives 423.0_2-2 Conc. (ppm) 68.97 0.31 3.37 635000.00 163.62 559.87 BD 1.29 2.90 31.42DL 0.74 1.12 0.55 11.55 0.06 0.99 0.83 0.43 2.45 6.12Precision(%) 8.86 152.04 41.07 3.25 3.32 3.31 21.36 38.81 10.68

St Ives 423.0_3-3 Conc. (ppm) 45.84 BD 18.17 635000.00 129.10 809.28 BD 1.20 4.19 26.83DL 0.54 1.25 0.64 10.16 0.05 0.21 0.67 0.51 3.07 6.01Precision(%) 14.81 14.55 2.82 3.01 2.98 22.04 28.26 10.21

Golden Mile Chron. Samples Synvolcanic sulfide LG106_1-1 Conc. (ppm) 7.37 BD 5039.45 635000.00 26.70 1122.73 2.85 6.84 319.06 30.34DL 0.80 1.65 1.01 16.50 0.15 0.42 1.69 0.77 1.29 13.94Precision(%) 11.48 10.46 6.08 25.83 7.50 24.99 14.09 14.29 19.68

Golden Mile Chron. Samples Synvolcanic sulfide LG106_1-2 Conc. (ppm) 48.60 99.07 182.82 635000.00 42.51 1089.01 6.51 70.62 1127.11 36.75DL 0.98 1.78 1.23 18.27 0.12 0.39 1.70 0.72 1.18 11.84Precision(%) 16.44 19.97 18.51 7.73 12.64 8.69 32.72 19.51 12.77 16.10

Golden Mile Chron. Samples Synvolcanic sulfide LG106_4-1 Conc. (ppm) 16.50 BD 8.37 635000.00 0.05 1289.84 1.75 1.15 BD 29.76DL 0.94 1.56 1.06 12.55 0.10 0.32 1.49 0.64 1.18 8.68Precision(%) 17.10 16.41 2.69 79.11 2.68 33.60 27.33 12.50

376

Sample No

423.0_1-4

423.0_2-1

423.0_2-2

423.0_3-3

LG106_1-1

LG106_1-2

LG106_4-1

Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2380.05 1.02 0.12 3.81 0.29 0.11 2.58 0.10 0.01 0.06 0.06 0.02 0.06 0.03 0.01 0.02

39.81 27.32 15.40 14.09 35.47 25.02 19.54 32.55 27.17 5.19 5.47 32.97283.28 BD 0.78 BD 3.87 0.81 BD 407.37 7.69 0.49 BD 0.20 9.98 0.35 8.81 4.50

0.17 4.53 0.45 21.05 0.93 0.41 11.52 0.50 0.07 0.39 0.24 0.12 0.17 0.11 0.04 0.0630.78 36.08 20.50 31.50 19.98 24.19 44.43 34.32 18.10 30.47 28.35 27.72

0.06 BD 0.16 BD 0.76 BD BD 0.75 0.02 BD BD BD 1.01 0.15 BD BD0.03 0.75 0.13 3.69 0.14 0.12 1.77 0.10 0.01 0.04 0.05 0.02 0.04 0.01 0.01 0.01

35.14 33.35 9.35 24.96 41.93 6.90 9.380.02 BD 0.20 2.74 0.80 BD BD BD 0.02 0.11 BD 0.02 1.77 0.28 BD 0.020.03 0.78 0.14 3.30 0.14 0.14 1.88 0.17 0.01 0.05 0.06 0.02 0.05 0.02 0.01 0.01

80.55 42.67 54.81 11.45 49.57 37.92 50.26 10.30 13.63 66.0417.42 BD 0.31 1.27 0.48 0.21 BD 4.97 0.03 BD BD 0.05 3.83 0.49 0.57 0.280.02 0.86 0.18 3.56 0.19 0.09 2.19 0.14 0.02 0.06 0.07 0.02 0.05 0.02 0.01 0.01

29.49 26.20 114.77 17.80 25.18 20.84 30.24 22.64 13.26 8.39 31.67 31.3032.48 BD 2.14 BD 3.29 3.50 BD 0.63 1.37 0.16 1.21 BD 22.62 12.33 0.05 0.230.04 1.06 0.16 5.57 0.33 0.15 4.42 0.21 0.02 0.08 0.10 0.03 0.06 0.02 0.02 0.02

18.91 12.27 10.16 11.51 21.92 12.52 39.17 78.79 11.38 11.16 31.82 25.093.53 BD 2.41 7.41 1.67 2.57 BD 0.06 0.09 BD 0.25 BD 16.46 10.41 BD BD0.05 1.30 0.28 6.03 0.34 0.23 3.79 0.19 0.02 0.07 0.05 0.03 0.05 0.03 0.02 0.02

37.95 11.55 31.66 10.75 12.72 137.61 23.37 22.71 11.48 10.580.85 BD 0.43 BD 1.54 BD BD BD BD 0.12 0.05 BD 2.32 0.63 0.02 0.010.03 0.94 0.25 6.20 0.28 0.16 3.10 0.14 0.02 0.07 0.05 0.03 0.05 0.02 0.02 0.01

23.35 26.85 9.06 32.50 46.02 13.35 10.62 48.19 71.87

377

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82

New Celebration Stage I Porphyry 1213279_5-1 Conc. (ppm) 5820.78 892.40 155.75 325633.11 255.56 1939.55 467.35 253.02 BD BDDL 16.73 64.17 35.02 466.06 3.90 16.78 51.60 30.37 39.05 321.03Precision(%) 20.04 20.26 20.94 18.66 19.53 18.01 24.86 20.16

New Celebration Stage I Porphyry 1213279_5-2 Conc. (ppm) 2579.06 568.53 40.87 19865.24 BD 362.70 613.88 114.02 BD BDDL 8.01 24.12 22.71 296.54 2.19 10.89 30.29 9.42 17.44 156.70Precision(%) 21.71 23.14 34.40 21.93 22.54 23.12 28.12

New Celebration Stage I Porphyry 1213279_5-3 Conc. (ppm) 154.21 135.68 BD 1596.21 BD BD 678.68 BD BD BDDL 51.22 125.90 105.69 1077.47 11.98 30.73 110.98 54.58 106.22 970.15Precision(%) 29.52 43.55 34.71 27.15

New Celebration Stage II Facture 1213359_1-1 Conc. (ppm) 17.88 BD BD 384965.50 176.45 735.44 78.95 BD BD BDDL 12.62 18.71 16.75 198.98 1.88 6.26 17.28 10.72 18.97 164.06Precision(%) 55.93 43.80 43.85 43.86 49.24

New Celebration Stage II Facture 1213359_2-1 Conc. (ppm) 486.59 BD BD 583068.25 16.22 57.43 145.22 BD BD BDDL 10.64 28.55 16.52 230.92 2.54 11.42 28.12 13.41 21.40 195.29Precision(%) 30.04 27.10 28.85 29.47 31.64

New Celebration Stage II Facture 1213359_3-1 Conc. (ppm) BD BD BD 363.12 BD BD 120.94 BD BD BDDL 18.80 33.60 25.22 328.24 3.18 11.50 33.50 27.00 30.10 314.27Precision(%) 40.01 26.79

New Celebration Stage II Facture 1213359_4-1 Conc. (ppm) BD BD BD 384710.90 32.83 99.99 230.32 BD BD BDDL 80.46 136.63 103.39 1215.46 10.64 40.49 122.50 64.21 86.58 953.85Precision(%) 17.44 26.11 26.37 26.25

New Celebration Stage II Contact 1250_12-18_5-1 Conc. (ppm) 8.24 BD BD 248826.33 300.46 2893.68 499.87 BD 18.89 BDDL 12.30 27.27 19.34 318.21 2.32 7.05 24.18 19.63 22.70 184.15Precision(%) 70.11 20.12 20.76 20.26 21.74 51.46

Golden Mile Fimiston Depth D14_1-1 Conc. (ppm) BD BD 9664.44 200477.95 BD 7.24 1226.60 203.21 BD BDDL 4.93 11.68 5.87 87.59 0.54 3.39 6.59 3.99 27.30 71.57Precision(%) 403.41 36.42 36.41 48.32 47.34 38.16

Golden Mile Fimiston Depth D14_1-2 Conc. (ppm) 54.05 BD BD 2314245.17 69.70 488.69 2739.54 120.02 8207.99 585.64DL 16.71 28.89 26.77 393.65 2.78 9.25 36.42 15.59 108.19 261.56Precision(%) 33.91 26.90 30.66 27.67 29.91 36.22 29.79 32.79

Golden Mile Fimiston Depth D14_1-3 Conc. (ppm) 5256.80 BD 75901.98 5361515.94 343.04 3077.14 4523.14 3649.57 13964.05 BDDL 199.34 271.15 177.53 2855.40 19.64 66.76 264.03 118.82 719.59 1794.52Precision(%) 17.75 15.72 12.54 16.95 14.62 16.12 13.32 16.40

Golden Mile Chron. Samples Fimiston Stage III LGX_1-1 Conc. (ppm) BD BD BD BD BD BD 913.89 BD BD BDDL 7.17 7.17 4.43 114.25 0.55 1.27 6.63 2.37 20.99 47.65Precision(%) 26.67

Golden Mile Chron. Samples Fimiston Stage III LGX_1-2 Conc. (ppm) 73.04 BD BD 1908.38 BD BD 384.75 12.81 14.97 BDDL 4.15 4.10 2.44 40.88 0.27 1.13 3.49 1.98 11.96 34.29Precision(%) 19.41 16.28 22.24 36.73

Golden Mile Chron. Samples Fimiston Stage III LGX_1-3 Conc. (ppm) 94.63 BD BD 2076.82 BD BD 664.65 11.34 BD 122.42DL 3.01 5.38 2.87 40.38 0.35 1.90 4.87 1.80 16.38 40.61Precision(%) 16.05 16.05 15.77 22.81 26.54

378

Sample No

1213279_5-1

1213279_5-2

1213279_5-3

1213359_1-1

1213359_2-1

1213359_3-1

1213359_4-1

1250_12-18_5-1

D14_1-1

D14_1-2

D14_1-3

LGX_1-1

LGX_1-2

LGX_1-3

Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U238

9.19 BD 68921.27 BD BD 34.35 134.45 2354.04 BD BD 900000.00 1.03 191.29 164.47 BD BD1.92 40.65 9.45 234.47 9.23 6.40 98.72 7.33 0.34 2.20 5.12 0.81 2.61 1.34 0.60 0.66

25.41 24.30 25.59 39.03 20.13 24.50 41.66 22.83 21.296.85 BD 69547.83 BD BD BD BD 771.40 BD BD 900000.00 BD 35.21 5.06 0.22 0.440.74 17.77 3.89 87.61 4.37 3.76 44.54 4.35 0.32 1.45 0.00 0.65 1.21 0.67 0.21 0.36

30.15 22.02 20.83 22.27 57.44 25.26 67.53 58.528.85 BD 57386.79 BD BD BD BD 77.86 BD BD 900000.00 BD 26.61 4.94 BD BD7.02 86.40 21.33 464.75 24.00 19.08 220.66 16.10 2.14 8.46 13.13 3.29 8.17 3.37 2.67 1.95

50.87 26.41 25.23 25.42 29.71 48.01BD BD 41496.53 BD BD BD BD BD BD BD 900000.00 BD 52.51 6.73 BD BD

0.42 12.68 3.38 62.59 3.86 2.77 42.21 2.42 0.27 1.20 0.00 0.45 1.38 0.42 0.31 0.2446.86 61.45 45.41 47.52

45.43 BD 76126.91 BD BD BD BD BD 2.01 32.01 900000.00 BD 40.65 44.88 1.73 0.730.61 21.29 4.90 96.20 4.91 3.01 54.18 2.45 0.31 1.77 0.00 0.67 1.66 0.57 0.37 0.29

34.11 30.47 57.45 30.79 37.66 29.06 28.42 46.40 43.9553.50 BD 87915.76 BD BD BD BD 1166.81 BD BD 900000.00 BD 87.17 288.93 1.79 3.311.43 18.69 5.91 96.64 7.32 4.59 56.67 4.31 0.43 1.77 2.08 1.07 1.62 0.93 0.36 0.46

30.02 17.07 17.15 16.37 17.17 20.81 22.77 19.9726.31 BD 70115.66 BD BD 16.56 BD BD BD BD 900000.00 BD 315.25 31.55 BD BD2.91 87.45 16.66 544.65 22.70 14.38 184.83 6.84 1.48 9.43 11.76 4.07 8.56 2.53 1.52 1.38

98.84 15.37 40.04 14.57 15.25 21.330.23 BD 79358.52 BD BD BD BD BD BD BD 900000.00 BD 2.24 5.23 BD BD0.00 18.09 15.63 118.91 6.45 3.08 61.09 3.99 0.25 1.43 0.00 0.82 1.58 0.94 0.41 0.38

52.58 21.02 25.10 38.21 23.89BD BD 70228.55 BD 2.34 BD 20.05 BD 0.25 BD 900000.00 BD 2.47 0.29 BD BD

0.13 8.31 1.39 41.25 1.97 0.99 24.23 0.86 0.12 0.57 0.00 0.19 0.37 0.20 0.07 0.1147.89 53.33 67.91 58.15 50.26 39.98 57.29

BD BD 76319.29 BD 11.85 21.76 4329.11 BD BD BD 900000.00 BD 44.13 5.97 BD BD1.16 34.29 7.29 157.04 6.36 4.12 98.49 6.35 0.69 1.70 96145.51 1.09 1.61 1.15 0.32 0.39

37.26 35.96 30.70 28.29 37.66 29.02 33.43BD BD 54802.29 BD BD 55.00 2473.30 BD 7.03 52.18 900000.00 BD 171.37 40.88 BD BD

6.64 336.87 51.23 1287.53 63.50 24.73 785.29 41.21 1.56 16.77 30.65 8.28 11.11 5.52 3.12 3.7913.03 28.92 24.48 22.91 46.46 14.03 17.46 17.67

BD BD 43290.82 BD 1.50 1.55 BD BD BD BD 900000.00 BD BD BD BD BD0.16 6.50 1.02 35.01 1.38 0.72 15.32 0.97 0.11 0.55 0.00 0.18 0.23 0.17 0.05 0.08

26.64 42.67 31.61 28.700.11 BD 50791.22 BD 4.15 2.63 BD 0.74 BD 0.52 900000.00 BD 0.83 BD BD BD0.08 4.85 1.18 18.04 0.94 0.36 9.19 0.39 0.05 0.15 0.00 0.09 0.22 0.12 0.04 0.06

43.11 15.46 22.20 21.12 45.47 26.32 17.65 21.740.41 BD 44887.93 BD 2.69 2.14 416058.54 71.78 BD BD 900000.00 0.57 14.59 BD BD 0.080.12 4.60 1.75 24.34 1.02 0.78 11.66 0.44 0.06 0.37 0.00 0.10 0.24 0.10 0.07 0.06

24.24 17.13 23.72 24.30 22.44 16.81 18.66 20.94 37.00 40.33

379

Location Event Style Sample No Ti49 Cr53 Mn55 Fe57 Co59 Ni60 Cu65 Zn66 As75 Se82Golden Mile Chron. Samples Fimiston Stage III LGX_1-4 Conc. (ppm) 12.44 BD BD 5144.76 BD BD 50788.53 7689.88 24290.86 83.20

DL 4.46 6.86 3.84 60.03 0.47 1.68 5.19 3.07 15.09 44.88Precision(%) 34.27 33.19 34.06 36.04 36.58 42.17

Golden Mile Western Lode Lake View LV46_3-1 Conc. (ppm) 111.34 6.85 15.29 17579.25 2.62 387.41 433.63 155.87 253.62 BDDL 1.52 2.34 1.01 18.33 0.16 0.59 1.78 0.94 5.75 19.43Precision(%) 22.96 26.26 20.01 15.50 19.01 21.77 15.99 22.27 19.33

Golden Mile Western Lode Lake View LV46_3-2 Conc. (ppm) 6.96 BD BD 251542.01 350.95 12.52 297.03 BD 275.76 BDDL 2.05 5.65 4.41 64.75 0.45 2.50 5.57 2.28 19.35 50.00Precision(%) 49.80 42.37 43.87 44.47 44.73 9292.65 42.82

Golden Mile Eastern Lode Oroya OR3_3 Conc. (ppm) BD BD BD 1671.18 2.16 527.38 203.52 BD BD BDDL 4.30 9.79 6.54 67.71 0.55 1.04 6.34 3.43 20.92 88.77Precision(%) 98.07 29.55 24.46 26.91

380

Sample NoLGX_1-4

LV46_3-1

LV46_3-2

OR3_3

Zr90 Mo95 Ag107 Cd111 Sn118 Sb121 Te125 Ba137 La139 W182 Au197 Tl205 Pb208 Bi209 Th232 U2380.27 BD 38653.57 47.67 1.63 6044.99 215381.00 9.80 BD BD 900000.00 0.28 10.65 0.81 BD BD0.20 5.52 2.78 26.71 1.24 0.67 26.59 0.94 0.12 0.58 0.00 0.20 0.20 0.13 0.08 0.06

45.17 27.23 33.41 37.80 35.72 37.14 26.28 29.87 44.51 31.39 37.171.33 BD 46129.25 BD 20.92 1.61 31.10 2.41 0.03 1.68 900000.00 BD 7.01 0.05 BD BD0.00 1.91 0.37 8.67 0.48 0.26 5.12 0.28 0.03 0.09 0.00 0.06 0.09 0.03 0.02 0.02

22.96 16.32 38.62 21.79 17.86 27.98 51.21 22.10 17.19 19.82 39.09BD BD 39235.27 BD BD BD 26.91 BD BD BD 900000.00 BD 8.70 BD BD BD

0.23 6.57 1.00 35.62 1.32 0.74 14.48 0.76 0.12 0.44 0.00 0.16 0.29 0.10 0.10 0.0844.57 51.37 56.62 43.16

BD BD 106435.99 BD 3.59 159077.09 530234.54 1.78 BD BD 900000.00 0.44 2400.31 0.41 BD BD0.21 7.14 1.45 37.97 1.68 0.79 13.08 0.82 0.14 0.59 6.18 0.18 0.36 0.16 0.13 0.07

26.88 26.06 24.94 24.18 39.12 24.01 34.80 25.26 33.12

381

APPENDICES

382

APPENDIX 9 Whole-Rock Geochemistry –

Methodology And Results

Lab Number Sample Number Drill Hole From (m) To (m) Comment Method SiO2 (%) Al2O3

(%)Fe2O3

(%)MgO (%) CaO (%)

Na2O (%)

K2O (%)

TiO2

(%)P2O5

(%)NCGCH-001 HBW_1250_12-018 HBW_1250_12 264.20 264.40 Contact Style Mineralisation 4A 10.90 4.71 12.19 17.79 21.63 0.14 2.50 0.35 0.02NCGCH-002 HBW_1250_12-019 HBW_1250_12 264.50 264.60 Contact Style Mineralisation 4A 10.93 4.46 11.38 17.59 22.44 0.25 2.19 0.29 0.01NCGCH-003 JD0475-024 JD0475 223.60 223.80 Contact Style Mineralisation 4A 57.46 11.39 4.06 4.21 6.17 6.67 0.20 0.48 0.05NCGCH-004 1213372 JD0433 168.80 168.90 Contact Style Mineralisation 4A 42.78 9.60 10.42 13.90 5.64 0.94 5.21 0.39 0.01NCGCH-005 JD0475-021 JD0475 208.90 209.00 Porphyry Style Mineralisation 4A 51.40 13.07 5.56 5.16 5.50 6.25 1.54 0.53 0.21NCGCH-006 JD0475-022 JD0475 211.70 211.90 Porphyry Style Mineralisation 4A 54.90 11.16 5.01 5.04 6.87 5.93 0.72 0.44 0.24NCGCH-007 HBW_1250_12-007 HBW_1250_12 213.90 214.00 Porphyry Style Mineralisation 4A 62.12 14.65 5.20 2.27 3.03 7.14 0.76 0.49 0.10NCGCH-008 1213374 JD0433 172.20 172.30 Porphyry Style Mineralisation 4A 56.21 9.80 4.22 4.97 7.80 5.61 0.24 0.37 0.04NCGCH-009 1213373 JD0433 169.50 169.70 Porphyry Style Mineralisation 4A 46.54 12.99 7.30 8.27 6.23 5.69 2.46 0.59 0.17NCGCH-010 1213297 JD0433 192.00 192.10 Porphyry Style Mineralisation 4A 54.03 14.39 5.54 4.93 5.45 8.25 0.49 0.65 0.20NCGCH-011 1213282 JD236 130.25 130.60 Porphyry Style Mineralisation 4A 49.70 13.76 6.87 6.31 5.68 6.76 1.74 0.60 0.26NCGCH-012 HBW_1250_12-022 HBW_1250_12 306.20 306.60 Fracture Style Mineralisation 4A 69.14 14.34 1.41 0.80 1.94 4.73 4.20 0.19 0.14NCGCH-013 HBW_1250_12-023 HBW_1250_12 307.10 307.30 Fracture Style Mineralisation 4A 65.69 13.33 1.48 1.55 3.25 4.79 3.97 0.17 0.39NCGCH-014 HBW_1250_12-024 HBW_1250_12 309.60 309.80 Fracture Style Mineralisation 4A 21.38 6.62 12.14 16.10 17.96 0.11 3.82 0.31 0.01NCGCH-015 1213256 HBC_1225_13 231.30 231.50 Fracture Style Mineralisation 4A 65.57 18.76 1.06 0.74 1.01 7.71 2.03 0.21 0.16NCGCH-016 1213356 JD433 137.80 137.90 Fracture Style Mineralisation 4A 69.68 15.16 0.98 0.73 1.29 6.34 3.62 0.19 0.11NCGCH-017 1213245 HBC_1225_13 131.10 131.40 Mylonite Style Mineralisation 4A 51.91 11.83 7.09 4.60 6.72 6.22 1.38 0.59 0.12NCGCH-018 1213221 Pit Sample Mylonite Style Mineralisation 4A 44.06 12.13 9.69 6.56 8.36 1.64 4.02 0.56 0.06NCGCH-019 1213248 HBC_1225_13 136.20 136.50 Mylonite Style Mineralisation 4A 44.70 12.84 14.98 5.89 4.17 5.10 3.74 1.60 0.42NCGCH-020 HBC_1450_12-002 HBC_1450_12-002 282.70 282.90 Least Altered M2 Porphyry 4A 71.03 15.24 1.34 0.63 1.36 7.00 1.25 0.19 0.09NCGCH-021 HBC_1450_12-003 HBC_1450_12-003 281.40 281.50 Least Altered M2 Porphyry 4A 72.11 14.58 1.55 0.66 1.31 5.87 1.52 0.18 0.09NCGCH-022 Pit Sample Least Altered M2 Porphyry 4A 74.21 13.63 1.14 0.76 1.10 5.51 1.57 0.18 0.17NCGCH-023 Pit Sample Least Altered M1 Porphyry 4A 51.28 12.36 6.65 6.66 6.15 5.12 2.32 0.58 0.34NCGCH-024 HBW_1250_12-029 HBW_1250_12 344.50 344.80 Least Altered Ultramafic 4A 44.13 8.05 11.13 21.34 7.22 0.26 1.04 0.33 0.04NCGCH-025 HBW_1250_12-030 HBW_1250_12 346.80 347.00 Least Altered Ultramafic 4A 41.66 6.82 10.17 21.59 7.97 0.63 0.35 0.28 0.04NCGCH-026 133573 Pit Sample Least Altered Ultramafic 4A 42.26 8.16 12.49 20.99 6.98 0.31 2.55 0.34 0.04NCGCH-027 1213288 JD433 186.40 186.60 Least Altered Ultramafic 4A 38.22 4.24 9.10 29.04 1.91 0.06 0.14 0.17 0.02NCGCH-028 1213266 JD236 76.25 76.50 Least Altered Hanging Wall Dolerite 4A 47.16 14.24 13.49 7.64 9.70 2.30 0.11 0.90 0.08NCGCH-029 JD0475-002 JD0475 82.00 82.30 Least Altered Hanging Wall Dolerite 4A 46.26 14.16 12.66 10.89 9.78 1.81 0.28 0.70 0.05NCGCH-030 JD0475-003 JD0475 95.50 96.00 Least Altered Hanging Wall Dolerite 4A 45.80 14.81 13.60 10.63 8.38 1.99 0.23 0.71 0.06NCGCH-031 HBW1250_12-001 HBW1250_12 183.00 183.10 Least Altered MgB 4A 42.39 12.68 15.17 4.81 8.31 2.99 2.16 1.73 0.24NCGCH-032 HBW1250_12-002 HBW1250_12 186.20 186.50 Least Altered MgB 4A 44.94 13.00 15.77 5.33 8.16 2.04 1.29 1.71 0.24NCGCH-033 HBW_1250_12-029 HBW_1250_12 344.50 344.80 Duplicates 4A 44.86 7.83 10.80 21.12 7.68 0.25 0.76 0.33 0.02NCGCH-034 1213245 HBC_1225_13 131.10 131.40 Duplicates 4A 55.37 13.52 7.93 3.64 3.05 7.67 0.50 0.87 0.27

RE NCGCH-027 Repeat 4A 37.94 4.18 9.20 29.25 1.93 0.06 0.13 0.17 0.02RRE NCGCH-027 Reject Repeat 4A 38.09 4.21 9.31 29.30 1.90 0.05 0.13 0.17 0.02STANDARD SO-18/R-2a/CSB 4A 57.74 14.34 7.82 3.30 6.37 3.80 2.14 0.68 0.83STANDARD SO-18/R-2a/CSB 4A 58.14 14.16 7.63 3.34 6.39 3.70 2.17 0.69 0.83

383

Lab Number

NCGCH-001NCGCH-002NCGCH-003NCGCH-004NCGCH-005NCGCH-006NCGCH-007NCGCH-008NCGCH-009NCGCH-010NCGCH-011NCGCH-012NCGCH-013NCGCH-014NCGCH-015NCGCH-016NCGCH-017NCGCH-018 NCGCH-019NCGCH-020NCGCH-021NCGCH-022 NCGCH-023 NCGCH-024NCGCH-025NCGCH-026 NCGCH-027NCGCH-028NCGCH-029NCGCH-030NCGCH-031NCGCH-032NCGCH-033NCGCH-034

RE NCGCH-027RRE NCGCH-027STANDARD STANDARD

MnO (%)

Cr2O3

(%)Ba

(ppm)Ni

(ppm)Sc

(ppm)LOI (%)

TOT/C (%)

TOT/S (%)

SUM (%)

0.18 0.46 275 1066 33 28.60 8.78 2.85 99.640.17 0.37 265 1023 28 29.40 8.94 3.31 99.640.06 0.03 743 111 9 9.00 2.53 1.92 99.880.14 0.22 495 221 26 10.50 2.90 0.67 99.850.07 0.03 380 103 15 10.60 2.25 0.55 99.980.09 0.03 251 66 13 9.50 2.76 0.67 99.970.04 0.01 147 23 6 4.20 1.09 1.54 100.030.05 0.04 758 115 10 10.40 3.17 1.59 99.850.09 0.08 655 237 14 9.30 2.64 1.67 99.810.06 0.03 413 91 12 5.90 1.55 2.18 99.970.08 0.03 850 128 17 7.90 2.18 1.56 99.800.01 0.00 2305 14 2 2.80 0.63 0.45 99.980.02 0.00 5022 10 4 4.50 1.08 0.52 99.730.18 0.33 808 749 24 20.60 6.61 4.18 99.750.01 0.00 2801 11 2 2.40 0.28 0.42 100.000.01 0.00 1720 10 1 1.70 0.47 0.41 100.010.09 0.04 859 115 17 9.30 2.90 2.25 100.000.15 0.04 425 83 29 12.70 3.36 0.23 100.040.22 0.02 122 62 29 6.30 1.77 0.84 100.010.01 0.00 2945 10 1 1.50 0.45 0.39 99.990.01 0.00 2799 10 1 2.00 0.39 0.21 100.210.01 0.00 2135 10 2 1.50 0.35 0.44 100.030.09 0.05 501 122 17 8.30 2.37 0.55 99.980.15 0.37 240 1210 25 5.80 0.40 0.06 100.040.15 0.37 81 1248 23 9.70 1.77 0.30 99.900.15 0.40 155 907 27 5.10 0.61 0.03 99.900.10 0.37 41 1912 14 16.30 3.38 0.03 99.920.17 0.02 10 190 33 4.20 0.64 0.06 100.040.14 0.06 59 281 39 3.20 0.27 0.18 100.040.15 0.04 50 275 33 3.60 0.27 0.12 100.040.18 0.02 207 66 32 9.30 2.81 0.28 100.010.18 0.02 105 83 32 7.30 1.99 0.26 100.010.17 0.34 173 1028 25 5.70 0.56 0.01 100.010.12 0.02 245 71 15 7.00 2.13 1.45 100.00

0.10 0.38 42 1928 14 16.30 3.35 0.03 99.910.10 0.38 36 1948 14 16.00 3.41 0.03 99.920.38 0.55 530 3825 23 1.90 2.39 5.28 100.400.39 0.55 523 3816 23 1.90 2.40 5.28 100.43

384

Lab Number Sample Number Drill Hole From (m) To (m) Comment Method Cs (ppm)

Ga (ppm)

Hf (ppm)

Nb (ppm)

Rb (ppm)

Sn (ppm)

Sr (ppm)

NCGCH-001 HBW_1250_12-018 HBW_1250_12 264.20 264.40 Contact Style Mineralisation 4B 7.5 20.8 0.9 1.3 76.0 1 2043.2NCGCH-002 HBW_1250_12-019 HBW_1250_12 264.50 264.60 Contact Style Mineralisation 4B 5.9 15.3 0.6 1.1 68.9 1 2227.5NCGCH-003 JD0475-024 JD0475 223.60 223.80 Contact Style Mineralisation 4B 0.3 17.6 3.1 3.0 5.4 <1 563.9NCGCH-004 1213372 JD0433 168.80 168.90 Contact Style Mineralisation 4B 2.5 9.5 0.8 0.7 83.5 <1 521.4NCGCH-005 JD0475-021 JD0475 208.90 209.00 Porphyry Style Mineralisation 4B 3.7 17.5 3.2 2.9 36.8 <1 702.2NCGCH-006 JD0475-022 JD0475 211.70 211.90 Porphyry Style Mineralisation 4B 1.5 15.7 2.4 2.1 15.9 <1 751.4NCGCH-007 HBW_1250_12-007 HBW_1250_12 213.90 214.00 Porphyry Style Mineralisation 4B 1.9 17.0 3.8 5.3 30.2 2 189.7NCGCH-008 1213374 JD0433 172.20 172.30 Porphyry Style Mineralisation 4B 0.2 15.1 2.3 2.1 4.6 <1 845.7NCGCH-009 1213373 JD0433 169.50 169.70 Porphyry Style Mineralisation 4B 0.8 18.1 4.1 3.4 36.3 <1 796.8NCGCH-010 1213297 JD0433 192.00 192.10 Porphyry Style Mineralisation 4B 1.1 21.1 4.2 4.0 12.1 <1 639.3NCGCH-011 1213282 JD236 130.25 130.60 Porphyry Style Mineralisation 4B 4.6 17.3 2.9 2.2 48.2 <1 970.6NCGCH-012 HBW_1250_12-022 HBW_1250_12 306.20 306.60 Fracture Style Mineralisation 4B 0.7 20.5 3.4 1.4 53.7 <1 680.8NCGCH-013 HBW_1250_12-023 HBW_1250_12 307.10 307.30 Fracture Style Mineralisation 4B 0.8 21.0 3.4 1.5 52.0 <1 2874.5NCGCH-014 HBW_1250_12-024 HBW_1250_12 309.60 309.80 Fracture Style Mineralisation 4B 3.1 16.7 0.6 0.6 81.5 <1 1422.8NCGCH-015 1213256 HBC_1225_13 231.30 231.50 Fracture Style Mineralisation 4B 1.2 30.5 3.8 1.7 34.5 <1 618.5NCGCH-016 1213356 JD433 137.80 137.90 Fracture Style Mineralisation 4B 0.4 22.6 3.3 1.6 37.4 <1 530.2NCGCH-017 1213245 HBC_1225_13 131.10 131.40 Mylonite Style Mineralisation 4B 1.7 17.6 2.6 2.6 14.5 1 408.7NCGCH-018 1213221 Pit Sample Mylonite Style Mineralisation 4B 5.0 13.5 1.7 2.6 109.1 <1 295.8NCGCH-019 1213248 HBC_1225_13 136.20 136.50 Mylonite Style Mineralisation 4B 0.8 17.0 3.3 5.2 53.4 <1 155.8NCGCH-020 HBC_1450_12-002 HBC_1450_12-002 282.70 282.90 Least Altered M2 Porphyry 4B 0.7 22.0 3.5 1.7 25.3 <1 724.3NCGCH-021 HBC_1450_12-003 HBC_1450_12-003 281.40 281.50 Least Altered M2 Porphyry 4B 1.0 21.7 3.0 1.6 34.2 <1 831.7NCGCH-022 Pit Sample Least Altered M2 Porphyry 4B 1.0 20.7 2.8 1.4 27.8 <1 481.7NCGCH-023 Pit Sample Least Altered M1 Porphyry 4B 12.1 16.7 3.1 3.3 71.2 <1 513.6NCGCH-024 HBW_1250_12-029 HBW_1250_12 344.50 344.80 Least Altered Ultramafic 4B 7.8 9.1 0.6 0.6 34.3 <1 84.3NCGCH-025 HBW_1250_12-030 HBW_1250_12 346.80 347.00 Least Altered Ultramafic 4B 2.3 7.8 0.6 0.6 10.4 <1 252.3NCGCH-026 133573 Pit Sample Least Altered Ultramafic 4B 24.2 8.7 0.7 <.5 75.1 <1 31.7NCGCH-027 1213288 JD433 186.40 186.60 Least Altered Ultramafic 4B 0.9 4.9 <.5 <.5 4.3 <1 34.3NCGCH-028 1213266 JD236 76.25 76.50 Least Altered Hanging Wall Dolerite 4B 0.1 17.3 1.7 2.1 0.8 <1 112.8NCGCH-029 JD0475-002 JD0475 82.00 82.30 Least Altered Hanging Wall Dolerite 4B 1.2 17.1 1.5 1.7 8.2 <1 130.5NCGCH-030 JD0475-003 JD0475 95.50 96.00 Least Altered Hanging Wall Dolerite 4B 0.8 16.0 1.4 1.6 6.4 <1 127.2NCGCH-031 HBW1250_12-001 HBW1250_12 183.00 183.10 Least Altered MgB 4B 3.1 16.7 3.5 5.2 62.8 <1 111.0NCGCH-032 HBW1250_12-002 HBW1250_12 186.20 186.50 Least Altered MgB 4B 1.7 17.6 3.8 5.1 37.6 <1 122.5NCGCH-033 HBW_1250_12-029 HBW_1250_12 344.50 344.80 Duplicates 4B 5.9 7.7 0.7 0.7 22.9 <1 100.2NCGCH-034 1213245 HBC_1225_13 131.10 131.40 Duplicates 4B 3.3 17.3 2.7 4.2 14.6 <1 229.7

RE NCGCH-027 Repeat 4B 1 5 <.5 <.5 3.9 <1 37.6RRE NCGCH-027 Reject Repeat 4B 1 5.6 <.5 <.5 4.4 <1 37.2STANDARD SO-18 4B 6.9 18 10.3 20.1 27.5 13 410.8STANDARD SO-18 4B 7.3 17.8 10.2 20.1 29.2 13 409.8

385

Lab Number



Ta (ppm)

Th (ppm)

U (ppm)

V (ppm)

W (ppm)

Zr (ppm)

Y (ppm)

La (ppm)

Ce (ppm)

Pr (ppm)

Nd (ppm)

Sm (ppm)

Eu (ppm)

Gd (ppm)

Tb (ppm)

Dy (ppm)

Ho (ppm)

Er (ppm)

Tm (ppm)

Yb (ppm)

Lu (ppm)

<.1 0.8 0.4 367 10.5 20.7 9.4 2.3 5.1 0.71 3.6 1.2 0.44 1.52 0.27 1.41 0.29 0.84 0.12 0.73 0.14<.1 0.4 0.4 332 12.3 20.5 8.9 2.3 5.0 0.79 3.6 1.1 0.49 1.39 0.28 1.35 0.24 0.82 0.14 0.74 0.130.1 4.5 1.9 48 38.7 101.1 11.2 33.2 63.3 7.56 28.1 4.3 1.14 2.99 0.42 1.89 0.35 1.17 0.17 1.06 0.17<.1 0.5 0.5 185 38.7 23.9 8.0 1.9 3.9 0.59 2.6 0.8 0.23 0.93 0.20 1.29 0.28 0.81 0.13 0.92 0.130.2 3.8 1.0 129 23.4 97.1 12.9 28.6 58.2 7.34 29.8 5.0 1.43 3.55 0.46 2.16 0.41 1.25 0.17 1.18 0.170.1 3.2 0.7 92 18.4 79.4 12.2 21.0 43.1 5.47 23.2 4.1 1.12 2.99 0.44 1.97 0.35 1.09 0.15 1.03 0.170.4 3.9 1.1 61 16.4 123.7 10.0 18.6 34.8 4.25 16.3 2.7 0.84 2.53 0.39 1.68 0.34 0.87 0.13 0.93 0.140.1 4.5 4.0 57 45.8 76.9 9.6 24.0 49.0 6.30 24.9 4.2 1.07 2.83 0.35 1.77 0.30 0.85 0.14 0.89 0.120.2 7.1 9.9 91 49.4 117.4 10.5 37.5 72.9 9.05 35.5 5.4 1.42 3.70 0.49 1.78 0.32 0.92 0.15 0.81 0.150.3 6.5 2.3 59 55.5 135.7 16.1 38.0 75.6 9.33 34.5 5.7 1.59 4.08 0.61 2.84 0.53 1.45 0.21 1.26 0.220.1 7.2 1.9 111 28.1 92.1 14.4 38.4 71.4 8.97 35.5 5.8 1.44 4.12 0.57 2.51 0.49 1.37 0.19 1.32 0.22<.1 10.1 2.4 20 15.0 102.5 3.9 31.5 57.5 6.87 23.9 3.5 1.00 2.36 0.24 0.83 0.09 0.23 <.05 0.16 0.030.1 9.5 1.7 22 13.5 101.7 12.8 34.2 63.3 7.88 30.3 6.2 1.94 4.70 0.59 2.46 0.32 0.76 0.10 0.48 0.06<.1 0.6 1.2 376 4.8 16.3 7.1 4.0 7.5 0.93 4.0 1.0 0.52 1.22 0.20 1.20 0.24 0.70 0.10 0.66 0.100.1 12.0 2.5 25 15.6 128.8 4.2 41.3 76.0 8.61 31.4 4.6 1.08 2.46 0.25 0.89 0.11 0.23 <.05 0.24 0.02<.1 10.1 1.7 15 17.4 105.2 2.9 34.2 63.1 7.15 25.4 3.4 0.80 1.70 0.18 0.68 0.08 0.14 <.05 0.14 0.020.2 4.0 1.0 82 75.0 80.4 12.9 17.1 32.5 4.00 14.9 2.9 0.85 2.56 0.41 1.92 0.37 1.28 0.18 1.17 0.190.2 3.4 0.8 187 18.0 60.7 16.6 9.8 18.6 2.42 8.7 2.3 0.62 2.39 0.41 2.44 0.53 1.69 0.23 1.71 0.260.4 1.6 0.7 110 109.3 124.4 31.8 8.5 18.8 2.89 13.7 3.9 1.34 4.98 0.86 5.17 1.12 3.24 0.48 3.16 0.510.1 8.7 4.7 20 10.7 114.9 2.9 34.4 63.0 7.27 25.9 4.0 0.98 1.83 0.17 0.75 0.07 0.21 <.05 0.21 0.030.1 11.6 3.2 16 5.1 113.1 2.7 34.5 61.9 7.18 25.3 3.6 0.88 1.64 0.22 0.72 0.08 0.16 <.05 0.16 0.03<.1 8.6 3.3 25 14.6 97.0 3.9 31.4 57.6 6.62 24.1 3.7 0.90 2.14 0.24 0.88 0.12 0.24 <.05 0.20 0.030.2 4.3 1.1 130 6.7 108.6 17.1 33.5 71.3 9.39 38.6 6.4 1.68 4.81 0.65 2.80 0.53 1.47 0.21 1.26 0.20<.1 0.2 0.1 160 1.3 20.4 9.6 1.5 3.3 0.55 2.8 0.9 0.32 1.29 0.26 1.37 0.35 1.00 0.18 1.06 0.16<.1 0.1 <.1 131 3.3 18.6 8.2 1.1 2.2 0.32 1.3 0.6 0.30 1.08 0.20 1.23 0.29 0.94 0.14 0.99 0.13<.1 0.1 <.1 172 0.9 17.3 10.0 0.6 1.5 0.31 1.6 0.7 0.32 1.19 0.26 1.33 0.34 1.10 0.16 0.89 0.16<.1 <.1 <.1 79 2.7 10.2 4.6 0.7 1.4 0.20 1.2 0.3 0.14 0.60 0.09 0.87 0.14 0.56 0.07 0.45 0.080.2 0.2 0.1 260 0.8 56.8 22.6 3.3 8.2 1.44 6.9 2.4 0.85 3.14 0.58 3.49 0.83 2.39 0.36 2.24 0.390.2 0.2 0.1 223 1.0 41.2 18.1 2.7 6.5 1.09 5.2 1.8 0.82 2.47 0.43 2.92 0.64 1.87 0.28 1.88 0.290.2 0.3 0.1 227 0.5 43.9 17.9 2.7 7.1 1.10 5.5 1.7 0.83 2.66 0.49 3.11 0.70 1.90 0.30 1.97 0.270.5 1.3 0.7 347 57.7 134.1 32.5 8.6 19.8 2.82 13.4 3.7 1.42 4.97 0.94 5.48 1.28 3.53 0.56 3.33 0.510.4 1.7 0.5 293 18.7 132.9 32.7 10.0 22.7 3.45 15.7 4.4 1.57 5.29 0.94 5.64 1.21 3.54 0.54 3.43 0.56<.1 <.1 <.1 135 0.7 19.0 10.0 1.1 2.5 0.41 2.2 0.8 0.31 1.43 0.24 1.59 0.35 1.08 0.16 0.96 0.110.3 2.3 1.1 76 83.0 98.8 16.8 12.1 26.5 3.10 12.3 3.3 1.10 3.33 0.56 3.01 0.65 1.76 0.28 1.67 0.24

<.1 <.1 <.1 77 3.0 10.9 4.8 0.7 1.4 0.24 1.1 0.4 0.13 0.68 0.13 0.79 0.18 0.54 0.06 0.50 0.08<.1 0.1 <.1 78 2.5 10.5 4.8 0.6 1.5 0.23 0.7 0.3 0.12 0.55 0.12 0.75 0.20 0.51 0.08 0.37 0.097.6 10.3 16.4 194 16.1 282.6 33.5 13.1 27.7 3.36 13.7 3.1 0.91 3.00 0.54 2.92 0.64 1.90 0.30 1.77 0.287.8 10.2 16.5 208 16.2 284.2 34.1 12.8 29.0 3.58 14.5 3.0 0.96 3.00 0.54 2.90 0.66 1.92 0.28 1.84 0.28

386

Lab Number Sample Number Drill Hole From (m) To (m) Comment Method Mo (ppm)

Cu (ppm)

Pb (ppm)

Zn (ppm)

Ag (ppb)

Ni (ppm)

NCGCH-001 HBW_1250_12-018 HBW_1250_12 264.20 264.40 Contact Style Mineralisation 1F 1.27 73.08 20.33 132.3 907 1047.6NCGCH-002 HBW_1250_12-019 HBW_1250_12 264.50 264.60 Contact Style Mineralisation 1F 0.55 110.48 21.17 112.1 1465 917.8NCGCH-003 JD0475-024 JD0475 223.60 223.80 Contact Style Mineralisation 1F 0.58 6.73 7.50 35.7 299 114.5NCGCH-004 1213372 JD0433 168.80 168.90 Contact Style Mineralisation 1F 1.23 27.71 5.82 101.4 487 194.7NCGCH-005 JD0475-021 JD0475 208.90 209.00 Porphyry Style Mineralisation 1F 4.19 66.14 3.25 49.8 162 86.5NCGCH-006 JD0475-022 JD0475 211.70 211.90 Porphyry Style Mineralisation 1F 6.37 75.86 3.76 42.5 243 68.8NCGCH-007 HBW_1250_12-007 HBW_1250_12 213.90 214.00 Porphyry Style Mineralisation 1F 3.27 15.12 2.42 56.1 114 29.0NCGCH-008 1213374 JD0433 172.20 172.30 Porphyry Style Mineralisation 1F 3.19 33.72 7.11 35.4 627 121.7NCGCH-009 1213373 JD0433 169.50 169.70 Porphyry Style Mineralisation 1F 5.60 46.61 19.76 105.1 724 238.7NCGCH-010 1213297 JD0433 192.00 192.10 Porphyry Style Mineralisation 1F 0.37 45.62 11.71 35.9 745 76.4NCGCH-011 1213282 JD236 130.25 130.60 Porphyry Style Mineralisation 1F 1.59 103.58 5.54 44.0 353 118.9NCGCH-012 HBW_1250_12-022 HBW_1250_12 306.20 306.60 Fracture Style Mineralisation 1F 1.83 18.53 9.91 28.8 597 5.8NCGCH-013 HBW_1250_12-023 HBW_1250_12 307.10 307.30 Fracture Style Mineralisation 1F 3.12 8.40 8.51 34.8 156 3.8NCGCH-014 HBW_1250_12-024 HBW_1250_12 309.60 309.80 Fracture Style Mineralisation 1F 4.89 89.30 19.00 145.3 2235 696.2NCGCH-015 1213256 HBC_1225_13 231.30 231.50 Fracture Style Mineralisation 1F 2.10 1.68 3.07 10.5 77 4.1NCGCH-016 1213356 JD433 137.80 137.90 Fracture Style Mineralisation 1F 0.29 6.83 3.83 14.6 182 5.2NCGCH-017 1213245 HBC_1225_13 131.10 131.40 Mylonite Style Mineralisation 1F 2.36 40.83 6.97 49.0 1806 111.8NCGCH-018 1213221 Pit Sample Mylonite Style Mineralisation 1F 0.68 69.82 4.79 71.1 72 72.3NCGCH-019 1213248 HBC_1225_13 136.20 136.50 Mylonite Style Mineralisation 1F 0.94 66.15 9.14 83.1 293 71.0NCGCH-020 HBC_1450_12-002 HBC_1450_12-002 282.70 282.90 Least Altered M2 Porphyry 1F 1.15 13.52 3.47 17.1 253 2.9NCGCH-021 HBC_1450_12-003 HBC_1450_12-003 281.40 281.50 Least Altered M2 Porphyry 1F 2.21 7.88 16.24 44.2 57 1.6NCGCH-022 Pit Sample Least Altered M2 Porphyry 1F 0.80 6.28 10.62 24.0 113 3.0NCGCH-023 Pit Sample Least Altered M1 Porphyry 1F 8.25 66.43 5.67 69.2 89 104.4NCGCH-024 HBW_1250_12-029 HBW_1250_12 344.50 344.80 Least Altered Ultramafic 1F 0.11 82.97 1.45 35.4 48 609.9NCGCH-025 HBW_1250_12-030 HBW_1250_12 346.80 347.00 Least Altered Ultramafic 1F 1.23 39.89 3.52 25.1 31 454.4NCGCH-026 133573 Pit Sample Least Altered Ultramafic 1F 0.10 20.45 0.35 36.2 10 575.2NCGCH-027 1213288 JD433 186.40 186.60 Least Altered Ultramafic 1F 0.25 4.65 0.94 39.9 7 375.6NCGCH-028 1213266 JD236 76.25 76.50 Least Altered Hanging Wall Dolerite 1F 0.49 104.86 0.27 47.4 37 105.1NCGCH-029 JD0475-002 JD0475 82.00 82.30 Least Altered Hanging Wall Dolerite 1F 0.11 129.04 0.24 29.8 60 146.9NCGCH-030 JD0475-003 JD0475 95.50 96.00 Least Altered Hanging Wall Dolerite 1F 0.39 112.06 0.31 39.3 68 167.1NCGCH-031 HBW1250_12-001 HBW1250_12 183.00 183.10 Least Altered MgB 1F 0.45 80.79 1.41 108.9 124 56.3NCGCH-032 HBW1250_12-002 HBW1250_12 186.20 186.50 Least Altered MgB 1F 0.77 68.15 1.35 118.2 100 65.5NCGCH-033 HBW_1250_12-029 HBW_1250_12 344.50 344.80 Duplicate 1F 0.09 19.74 1.49 35.1 28 473.9NCGCH-034 1213245 HBC_1225_13 131.10 131.40 Duplicate 1F 0.63 83.21 6.16 54.1 748 63.4

RE NCGCH-027 Repeat 1F 0.25 4.50 0.96 40.5 5 392.4RRE NCGCH-027 Reject Repeat 1F 0.04 3.61 0.82 10.7 6 382.8STANDARD DS6 1F 11.28 127.21 28.78 144.9 281 24.4STANDARD DS6 1F 11.37 124.14 29.25 146.1 277 24.0

387

Lab Number



Co (ppm)

Mn (ppm)

As (ppm) Au (ppb) Cd

(ppm) Sb

(ppm) Bi

(ppm) Cr

(ppm) B

(ppm) Tl

(ppm) Hg

(ppm) Se

(ppm) Te

(ppm) Ge

(ppm) In

(ppm) Re

(ppb) Be

(ppm) Li

(ppm) Pd

(ppb)Pt

(ppb) Sample

(g)93.7 1469 1.8 3980.9 0.23 0.09 0.44 1917.7 <1 0.92 11 0.5 3.55 0.2 0.09 4 2.2 47.6 15 14 1580.4 1271 1.9 14926.2 0.25 0.08 0.58 1334.1 <1 0.70 13 0.7 3.03 0.2 0.06 2 1.3 35.4 15 8 3018.3 493 0.1 504.0 0.09 0.07 0.70 96.1 <1 0.05 <5 0.6 1.02 <.1 <.02 1 0.3 3.3 <10 <2 3053.5 1148 0.2 9128.4 0.10 0.17 0.10 1069.7 <1 0.87 10 0.3 0.23 0.4 0.06 4 2.3 37.2 <10 3 3023.7 617 0.2 747.1 0.08 0.07 0.19 215.3 <1 0.39 <5 0.3 0.12 0.1 0.03 1 0.7 17.3 <10 2 3018.6 792 0.1 847.9 0.05 0.08 0.24 175.3 <1 0.16 <5 0.3 0.11 0.2 0.02 3 0.4 11.6 <10 2 3017.6 368 1.2 955.3 0.07 0.22 0.27 29.6 <1 0.21 5 0.3 0.25 0.1 <.02 <1 0.1 17.8 <10 <2 3020.2 480 0.4 6464.2 0.08 0.22 0.22 96.0 <1 0.04 <5 0.6 0.33 <.1 0.02 1 0.7 4.0 <10 2 3035.6 771 0.4 13028.4 0.13 0.30 0.32 525.7 <1 0.40 <5 0.6 0.29 0.2 0.05 14 1.4 22.0 <10 4 3020.7 399 0.4 11441.5 0.07 0.11 0.56 112.4 <1 0.12 9 0.5 1.32 0.1 0.02 <1 0.3 8.1 16 2 3032.6 677 0.3 5511.9 0.09 0.06 0.71 202.3 <1 0.53 <5 0.6 0.40 0.2 0.04 3 0.9 20.5 <10 3 30

3.0 118 0.4 9313.7 0.04 0.05 0.45 10.2 1 0.03 11 0.1 0.18 <.1 <.02 <1 0.1 2.2 <10 <2 302.0 183 0.4 1426.9 0.06 0.09 0.22 12.1 <1 0.06 <5 0.2 0.21 <.1 <.02 <1 <.1 5.1 <10 <2 30

76.3 1430 0.6 33602.2 0.20 0.05 0.96 1888.8 <1 0.69 5 0.9 4.33 0.3 0.06 2 1.7 76.7 <10 9 301.7 69 0.2 347.9 0.04 0.04 0.10 11.5 2 0.05 <5 0.2 0.23 <.1 <.02 <1 0.1 6.3 15 <2 302.2 104 <.1 1298.3 0.06 0.04 0.28 14.4 1 <.02 9 0.1 0.18 <.1 <.02 <1 <.1 0.7 <10 3 30

26.5 795 2.4 16190.7 0.11 0.61 0.60 215.8 <1 0.10 6 0.9 2.26 0.1 0.04 1 0.4 10.6 <10 3 3036.1 1250 0.5 7.0 0.11 0.14 0.06 143.4 1 0.60 <5 0.2 0.05 0.1 <.02 1 0.5 29.5 17 9 3044.9 1765 2.0 1707.8 0.09 0.71 0.42 116.1 <1 0.63 13 0.6 0.29 0.2 0.08 2 1.3 20.8 <10 3 30

2.3 110 0.2 756.4 0.03 0.05 0.36 8.2 <1 0.03 12 0.1 0.06 <.1 <.02 <1 <.1 1.3 <10 4 302.0 105 0.2 113.4 0.05 0.04 0.14 8.7 1 0.03 <5 0.2 0.03 <.1 <.02 <1 0.1 2.0 <10 2 301.8 89 0.2 1061.1 0.03 0.06 0.24 10.8 1 0.04 <5 0.2 0.17 <.1 <.02 <1 0.1 3.2 17 2 30

28.6 805 0.1 10.5 0.07 0.05 0.12 394.1 1 0.87 <5 0.2 0.03 0.2 0.04 8 1.1 30.2 <10 3 3047.5 502 0.1 8.0 0.01 0.02 0.02 1912.4 <1 0.34 9 0.1 0.02 0.1 <.02 <1 <.1 45.5 <10 7 3045.0 930 1.4 12.0 0.04 0.02 0.12 1599.8 <1 0.10 <5 0.1 0.06 0.1 <.02 2 <.1 29.0 <10 4 3058.9 594 0.3 1.8 0.01 0.02 0.02 1739.8 <1 0.73 <5 0.1 <.02 0.1 <.02 1 <.1 75.6 <10 5 3033.1 852 0.2 3.8 0.03 0.68 <.02 1122.0 1 0.05 7 <.1 0.03 <.1 <.02 1 0.1 12.6 <10 6 3032.0 604 0.3 5.9 0.06 0.18 <.02 57.6 <1 <.02 6 0.1 <.02 0.1 <.02 1 <.1 19.8 <10 <2 3037.7 453 6.4 5.0 0.05 0.35 <.02 195.1 1 0.09 5 0.6 0.03 0.1 <.02 <1 <.1 19.8 <10 2 3042.8 557 1.1 7.8 0.04 0.21 <.02 180.1 <1 0.06 <5 0.5 0.02 0.1 <.02 2 <.1 24.7 <10 2 3039.2 1465 0.2 28.2 0.18 0.10 0.02 91.9 1 0.37 <5 0.3 0.09 0.1 0.03 2 <.1 29.4 10 <2 3038.3 1203 0.2 11.0 0.13 0.26 0.02 120.7 <1 0.34 <5 0.4 0.04 0.3 0.07 1 <.1 32.0 10 2 3040.0 533 0.1 4.0 0.02 0.03 0.03 1741.9 1 0.23 <5 <.1 0.03 0.1 <.02 1 0.1 47.0 <10 7 3026.3 954 5.6 6879.6 0.05 0.54 0.83 95.2 <1 0.14 7 0.6 1.01 0.1 0.05 <1 0.5 10.0 <10 <2 30

34.3 851 0.4 3.6 0.03 0.65 <.02 1202 1 0.04 <5 <.1 0.02 0.1 <.02 <1 0.1 14.1 <10 4 3033.5 812 <.1 5.7 0.02 0.03 <.02 1137.9 1 0.05 <5 <.1 0.02 <.1 <.02 <1 0.2 11.6 <10 2 3010.5 722 21.2 46.8 6.16 3.51 4.76 189.5 17 1.90 241 4.2 2.31 0.1 1.95 <1 2.4 15.7 162 42 3010.3 690 21.2 47.1 6.19 3.54 4.84 184.9 17 1.66 222 4.2 2.24 <.1 1.94 <1 2.3 16.1 167 44 30

388

852 East Hastings Street, Vancouver, BC Canada V6A 1R6 Phone (604) 253 3158 Fax (604) 253 1716 e-mail: [email protected]

Group 4A (e-mail versionv2.1) Revision Date: Feb 20, 2007

METHODS AND SPECIFICATIONS FOR ANALYTICAL PACKAGE GROUP 4A: WHOLE ROCK ANALYSIS BY ICP

Analytical Process

Receive Samples

Sort and Log Samples

Oven Dry at 60°C

Soils and Sediments Rocks and Core

Label and Sieve samples to –80 Mesh

Label, crush and pulverize to –150 Mesh

Weigh out 0.2 gm pulp into graphite crucibles. Add sample reference

materials and duplicates (rerun) to sequence.

Re-split

Mix with LiBO2/Li2B4O7

and fuse at 980°C

Dissolve bead in 0.5%

HNO3

Blanks, Calibration and Verification Standards

added to sequence

Analyse by ICP-ES Re-Analyze

No

Data correction and verification based on all

QC samples

Is data of acceptable

quality?

Data Entry, Checking and Analytical Report

Generation

Yes

Final Verification and

Certification

Comments

Sample Preparation

Soil or sediment is dried (60°C) and sieved to -80 mesh (-177 μm). Vegetation is dried (60°C) and pulverized or ashed (475°C). Moss-mat is dried (60°C), pounded and sieved to yield -80 mesh sediment. Rock and drill core is jaw crushed to 70% passing 10 mesh (2 mm), a 250 g aliquot is riffle split and pulverized to 95% passing 150 mesh (100 μm) in a mild-steel ring-and-puck mill.

Sample Digestion

A 0.2 g aliquot is weighed into a graphite crucible and mixed with 1.5 g of LiBO2/Li2B4O7 flux. Crucibles are placed in an oven and heated to 980°C for 30 minutes. The cooled bead is dissolved in 5% HNO3 (ACS grade nitric acid diluted in demineralised water). Calibration standards and reagent blanks are added to the sample sequence.

Sample Analysis

Sample solutions are aspirated into an ICP emission spectrograph (Spectro Ciros Vision) for the determination of the basic package consisting of the following 18 major oxides and elements: SiO2, Al2O3, Fe2O3, CaO, MgO, Na2O, K2O, MnO, TiO2, P2O5, Cr2O3, Ba, Nb, Ni, Sr, Sc, Y and Zr. The extended package also includes: Ce, Co, Cu, Ta and Zn. Loss on ignition (LOI) is determined for both packages by igniting a 1 g sample split at 950°C for 90 minutes then measuring the weight loss. Total Carbon and Sulphur are determined by the Leco method (Group 2A).

Quality Control and Data Evaluation

An Analytical Batch (1 page) comprises 36 samples. QA/QC protocol includes inserting a duplicate of pulp to measure analytical precision, a coarse (10 mesh) rejects duplicate to measure method precision (drill core samples only), an analytical blanks to measure background and an aliquot of in-house reference material SO-18 and CSC to measure accuracy in each analytical batch of 36 samples. STD SO-18 was certified in-house against Certified Reference Materials including CANMET SY-4 and USGS AGV-2, BCR-2, GSP-2 and W-2. Raw and final data from the ICP-ES undergoes a final verification by a British Columbia Certified Assayer who must sign the analytical report before release to the client.


Group 4B (e-mail versionv2.1) Revision Date: Feb 22, 2007

METHODS AND SPECIFICATIONS FOR ANALYTICAL PACKAGE GROUP 4B - WHOLE ROCK TRACE ELEMENTS BY ICP-MS

Analytical Process

Comments

Sample Preparation

All samples are dried at 60°C. Soil and sediment are sieved to -80 mesh (-177 μm). Moss-mats are disaggregated then sieved to yield -80 mesh sediment. Vegetation is pulverized or ashed (475°C). Rock and drill core is jaw crushed to 70% passing 10 mesh (2 mm), a 250 g riffle split is then pulverized to 95% passing 150 mesh (100 μm) in a mild-steel ring-and-puck mill.

Sample Digestion

A 0.2 g samples aliquot is weighed into a graphite crucible and mixed with 1.5 g of LiBO2/Li2B4O7 2 flux. The flux/sample charge is heated in a muffle furnace for 30 minutes at 980°C. The cooled bead is dissolved in 100 mL of 5% HNO3 (ACS grade nitric acid in de-mineralised water). An aliquot of the solution is poured into a polypropylene test tube. Calibration standards, verification standards and reagent blanks are included in the sample sequence.

Sample Analysis

Sample solutions are aspirated into an ICP mass spectrometer (Perkin-Elmer Elan 6000 or 9000) for the determination of the basic package consisting of the following 34 elements: Ba, Co, Cs, Ga, Hf, Nb, Rb, Sn, Sr, Ta, Th, Tl, U, V, W, Y, Zr, La, Ce, Pr, Nd, Sm, Eu, Gd, Tb, Dy, Ho, Er, Tm, Yb and Lu. A second sample split of 0.5 g is digested in Aqua Regia and analysed by ICP-MS (see Group 1DX) to determine: Au, Ag, As, Bi, Cd, Cu, Hg, Mo, Ni, Pb, Sb, Se, Tl and Zn.

Quality Control and Data Verification

An Analytical Batch comprises 36 samples. QA/QC protocol incorporates a sample-prep blank (G-1) carried through all stages of preparation and analysis as the first sample, a pulp duplicate to monitor analytical precision, a -10 mesh rejects duplicate to monitor sub-sampling variation (drill core only), a reagent blanks to measure background and an aliquot of in-house Standard Reference Materials like STD SO-18 to monitor accuracy. STD SO-18 was certified in-house against Certified Reference Materials including CANMET SY-4 and USGS AGV-2, G-2, BCR-2 and W-2.

Raw and final data undergo a final verification by a British Columbia Certified Assayer who signs the Analytical Report before it is released to the client.

Re-split

Re-analyse

Yes

No

Receive Samples


Soils & Sediments Vegetation

Label and Sieve samples to -80 Mesh

Rock and Core

Oven Dry at 60°C Ash at 475°C

Label, Crush & Pulverize to -150 mesh

Weigh out 0.2 g pulp into graphite crucibles. Sample

standards and pulp duplicates added to

sequence.

Mix with LiBO2/Li2B4O7 2 and fuse at 980°C

Add Calibration standards and reagent blanks to

sample sequence.

Sample solutions analysed by ICP-MS

LIMS system corrects data for interferences and drift. Operator reviews raw data

ICP-MS data and any other analyses combined as a final Analytical Report

Verification and Certification by a BC

Certified Assayer


quality?

Dissolve bead in 0.5% HNO3


Group 1F-MS (e-mail version1.2) Revision Date: Feb 20, 2007

METHODS AND SPECIFICATIONS FOR ANALYTICAL PACKAGE GROUP 1F-MS – ULTRATRACE ICP-MS ANALYSIS • AQUA REGIA

Analytical Process

Comments Sample Preparation

All samples are dried at 60°C. Soil and sediment are sieved to -80 mesh (-177 μm). Moss-mats are disaggregated then sieved to yield -80 mesh sediment. Vegetation is pulverized or ashed (475°C). Rock and drill core is jaw crushed to 70% passing 10 mesh (2 mm), a 250 g riffle split is then pulverized to 95% passing 150 mesh (100 μm) in a mild-steel ring-and-puck mill. Pulp splits of 0.5 g are weighed into test tubes, 15 and 30 g splits are weighed into beakers.

Sample Digestion

A modified Aqua Regia solution of equal parts concentrated ACS grade HCl and HNO3 and de-mineralised H2O is added to each sample (6 mL/g) to leach in a hot-water bath (~95°C) for one hour. After cooling the solution is made up to a final volume with 5% HCl. Sample weight to solution volume ratio is 0.5 g per 10 mL.

Sample Analysis

Solutions aspirated into a Perkin Elmer Elan 6000 or 9000 ICP mass spectrometer are analysed for the Basic package comprising 37 elements: Au, Ag, Al, As, B, Ba, Bi, Ca, Cd, Co, Cr, Cu, Fe, Ga, Hg, K, La, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb, Sc, Se, Sr, Te, Th, Ti, Tl, U, V, W and Zn. The Full package adds the 14 following elements: Be, Ce, Cs, Ge, Hg, In, Li, Nb, Rb, Re, Sn, Ta, Ta, Y, Zr, Pd and Pt. Larger sample splits are recommended for better analytical precision on elements subject to nugget effects (eg. Au, Pt).

Quality Control and Data Verification

An Analytical Batch (1 page) comprises 36 samples. QA/QC protocol incorporates a sample-prep blank (G-1) carried through all stages of preparation and analysis as the first sample, a pulp duplicate to monitor analytical precision, a -10 mesh rejects duplicate to monitor sub-sampling variation (drill core only), a reagent blank to measure background and an aliquot of in-house Standard Reference Materials like STD DS7 to monitor accuracy.

Raw and final data undergo a final verification by a British Columbia Certified Assayer who signs the Analytical Report before it is released to the client.

Re-split

Re-analyse

Yes

No

Receive Samples


Soils & Sediments Vegetation

Label and Sieve samples to -80 Mesh

Rock and Core

Oven Dry at 60°C Ash at 475°C

Label, Crush & Pulverize to -150 mesh

Weigh 0.5 g into test tubes, (15 or 30 g weighed into beakers) add duplicates and reference material to

the sample sequence

Add Aqua Regia acid mixture to test tubes and digest in boiling (>95°C)

water bath for 60 minutes.

Calibration standards and reagent blanks added to

sample sequence.

Sample solutions analysed by ICP-MS

LIMS system corrects data for interferences and drift. Operator reviews raw data

ICP data and any other analyses combined as a final Analytical Report

Verification and Certification by a BC

Certified Assayer


quality?

hydrothermal evolution of two stages of gold ...€¦ · neumayr under the auspices of the...

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