exploration report on reinfjord, …...the gabbro screen is conformable to the igneous layering of...
Post on 03-Jul-2020
1 Views
Preview:
TRANSCRIPT
EXPLORATION REPORT ON REINFJORD, LOKKARFJORD, AND
TAPPELUFT INTRUSIONS OF THE SEILAND IGNEOUS PROVINCE,
NORWAY
for
NORDIC MINING ASA
Markku Iljina GeoConsulting Tmi Dec 15, 2011
Table of Contents
1. Scope ................................................................................................................................................................1
2. Background .......................................................................................................................................................1
3. Geology .............................................................................................................................................................2
3.1. Reinfjord ...................................................................................................................................................3
3.2. Lokkarfjord ................................................................................................................................................4
3.3. Tappeluft ..................................................................................................................................................6
4. Field observations.............................................................................................................................................6
5. Whole-rock chemistry ................................................................................................................................... 17
5.1. Quality assessment ................................................................................................................................ 18
5.2. Theoretical background ......................................................................................................................... 18
5.3. Småvatna and Bonjikdalen sulphide chemistry ..................................................................................... 19
5.4. Scattered observations from Reinfjord intrusion .................................................................................. 23
5.5. Genesis of Reinfjord sulphides .............................................................................................................. 23
5.6 Lokkarfjord sulphide chemistry ............................................................................................................. 24
5.7. Tappeluft sulphide chemistry ................................................................................................................ 26
6. Conclusions .................................................................................................................................................... 26
6.1. Reinfjord ................................................................................................................................................ 26
6.1.1. Geophysical survey ........................................................................................................................ 26 6.1.2. Geological interpretation and ore genesis .................................................................................... 28 6.1.3. Recommendations ......................................................................................................................... 29
6.2. Lokkarfjord ............................................................................................................................................. 30
6.2.1. Geological interpretation and ore genesis .................................................................................... 30 6.2.2. Recommendations ......................................................................................................................... 30
6.3. Tappeluft ............................................................................................................................................... 31
7. Evaluation of the Seiland Igneous Province to host Ni-Cu-PGE sulphide deposits ....................................... 32
7.1. Geotectonic setting, age, and character of magmas ............................................................................. 32
7.2. Sulphide saturation ............................................................................................................................... 34
7.3. Encountered deposits and mineralisation indications .......................................................................... 34
7.4. Quantitative evaluation ......................................................................................................................... 35
8. References ..................................................................................................................................................... 36
APPENDIX 1 R factor calculations ...................................................................................................................... 38
APPENDIX 2 Field observations .......................................................................................................................... 40
Appendix 3 Petrohysical properties of the samples ......................................................................................... 45
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 1
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
1. Scope Markku Iljina GeoConsulting Tmi (MIGC) was engaged by Nordic Mining ASA to plan, execute
and report field exploration campaign on company’s pre-claims of Reinfjord, Tappeluft, and
Lokkarfjord locating in the counties of Finnmark and Troms (Fig. 1). The contract was confirmed
on May 2011 and the field operation itself was executed between 15th
and 27th
of August, 2011.
Student Outi Ahvenjärvi from the University of Oulu was employed by MIGC to assist in the
mission. In addition, a group of people from Nordic Mining and Trondheim University of Science
and Technology (NTNU) participated in the trip in Aug. 23rd
- 25th
, 2011. This Norwegian group
composed of Exploration Manager Mona Schanche (Nordic Mining), professor Rune Larsen, and
students Endre Nerhus Øen and Lars Anker-Rasch. NTNU student team stayed two weeks in
Reinfjord for geological mapping.
The contract included also arrangements for sample preparation, measurements of samples’
petrophysical properties, and haulage of samples to ALS Chemex assay laboratory in Piteå,
Sweden.
The reporting was agreed to compose of and discuss on the following subjects:
1. Field observations:
-Day-to-day sections of activities and observations
-Map illustration of observation points
-Tabled observation list with descriptions
-ArcView compatible Shape files of field observation
-ArcView compatible Shape files of petrophysical laboratory measurement results
- ArcView compatible Shape files of chemical assays
-Comments on petrophysical measurements
-Relationship of airborne EM anomalies and field observations
2. Geology section:
-Concise describtion of the geology of the Seiland Igneous Province
-Evaluation of the Seiland Igneous Province to host Ni-Cu-PGE deposits.
3. Assay results:
-Comments on analytical results.
4. Recommendations for further work
2. Background First exploration reports, including company reports and academic studies on nickel and copper
enrichments in Reinfjord and Lokkarfjord, derive from early ‘70ies. Later studies in Lokkarfjord as
ordered by Nordic Mining and made by Norwegian Geological Survey (NGU, Often and
Schiellerup, 2008) revealed the known sulphide dykes to have also high Platinum-Group Element
(PGE) contents as an sample returned with values of 0.80 % Ni, 0.72 % Cu, 608 ppb Pd, 166 ppb
Pt, and 49 ppb Au. For Reinfjord NGU reports 0.15 % Ni and 0.15 % Cu, but low PGE levels of
about few ppb. For Tappeluft base metal sulphides had been reported in an academic dissertation
(Roberts, 2007), but no attempt had been made to follow up the findings. The company had claimed
Lokkarfjord in 2010, and Reinfjord and Tappeluft in 2011.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 2
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 1. Geological map of the Seiland Igneous Province after Roberts (2007). Reinfjord, Tappeluft, and Lokkarfjord target areas indicated.
In Spring 2011 company contracted geophysical survey company, SkyTEM Surveys (SkyTEM), to
do helicopter geophysical measurements in Reinfjord and Lokkarfjord. These surveys measured
bedrock conductivity down to 500 m and total magnetic field. These surveys came back with
conductivity anomalies in Reinfjord but hardly any indications of conductors in Lokkarfjord. No
helicopter survey was done on Tappeluft.
The principal aim of the field exploration campaign reported here was to get bedrock information
from detected conductivity anomalies and re-sample known mineral enrichments. The academic
studies started by the NTNU students aim to produce further petrological information from
Reinfjord intrusion.
3. Geology Reinfjord, Tappeluft, and Lokkarfjord are ultramafic intrusions of the Seiland Igneous Province
(SIP), which in addition to ultramafic rocks is composed of various mafic and even alkaline igneous
rocks (Robins 1996, Roberts 2007, and Larsen 2011). The whole SIP is hosted by a nappe complex
of Norwegian Caledonides. SIP was emplaced and crystallized in a short time span of about 10 Ma,
560-570 Ma ago. Volumetrically largest mafic and ultramafic intrusions are aged to be formed in
LOKKARFJORD
TAPPELUFT REINFJORD
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 3
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
even shorter time span of only 4 Ma. The Province is interpreted to have extensional setting,
possibly in an intracontinental rift or in a back-arc setting.
Fig. 2. Bedrock (circles) and boulder (triangles) observation points and Reinfjord target areas on geological map. Day1,… refer to corresponding day descriptions in the text. Line A-B refers to cross-section depicted in Fig. 3. Map modified after Emblin 1985 to fit new field observations.
3.1. Reinfjord The following is based on descriptions made by Söyland Hansen (1971), Bennet (1971 and 1974),
Emblin (1985), and Bennett et al (1986). The Reinfjord intrusion has been intruded into layered
Langstrand gabbro found mainly on eastern and southern sides, and sedimentary garnet gneiss
found on the western side (Fig. 2). Main structural and lithological units of the intrusion are the
Layered Series (LS) and Central Series (CS) the latter been interpreted to have intrusive relationship
to the former. A Marginal Zone (MZ) has been developed between the LS and the enveloping
country rocks. In addition to these, a conspicuous Gabbro Screen is found as a giant slab inside in
the intrusion. This Gabbro Screen is also used to define Lower Layered Series and Upper Layered
Series and correspondingly the upper and lower Marginal Zones so that LS and MZ below the
screen are called ‘lower’, and those above as ‘upper’. In addition to upper and lower MZ, the
Northeast Marginal Zone has been defined; it separates CS from Langstrand gabbro in NE corner of
the intrusion.
The LS and CS are composed of olivine cumulates with various amounts of pyroxenes (wehrlite,
lherzolite, dunite). The prevailing pyroxene is clinopyroxene, which together with orthopyroxene
are commonly forming oikocrysts giving a poikilitic texture for the rock. The principal difference
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 4
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
between LS and CS lies in the amount of pyroxene the CS containing less pyroxene and being more
often dunite. The LS and CS are well-layered and layering is dipping to E-SE at shallow angle.
Fig. 3. Schematic cross-section over the Reinfjord intrusion approximately along the line A-B in Fig. 2. Modified after Bennett 1974. gn, garnet gneiss; gb, Langstrand Gabbro; MZ, Marginal Zone; umaf, ultramafic units.
The MZ is more heterogeneous in its lithology, structures, and textures. It is mainly ultramafic, but
more pyroxene rich (up to pyroxenite) than LS and contains also plagioclase in places making rock
gabbro and troctolite. Pyroxenitic and gabbroic pegmatites are present in MZ. It also contains
gabbro xenoliths sizing from dm to hundred meters. As an unit it represent a typical thick marginal
zone indicative of dynamic intrusion and extensive interaction of magma and partially melted
country rocks.
The gabbro Screen is an extensive sheet of Langstrand gabbro connecting the large gabbro territory
in the east to smaller gabbro body separating the Reinfjord intrusion and garnet gneiss in the west.
The Gabbro Screen is conformable to the igneous layering of the enveloping Reinfjord intrusion.
The strike length of the slab on present erosion surface is about 1.5 km while the thickness is
mapped to be 100-150 m (Fig. 2).
The relationship between various structural units of the ultramafic intrusion, garnet gneiss,
Langstrand gabbro, and gabbro screen is depicted in the Fig. 3.
As an entirety Reinfjord intrusion has vertical or steeply dipping contacts with enveloping country
rocks and is interpreted to plunge steeply to east or northeast. This also leads to imminent angular
discordance between the gently dipping layering of the intrusion and the country rock contacts. In
outcrop scale the contact zone is characterized by numerous gabbro rafts and tongues in the MZ
giving rise field relationship described as ‘interlayered’ in this field report.
3.2. Lokkarfjord
Lokkarfjord is rather small (c. 2 km2) ultramafic-mafic intrusion surrounded by younger gabbro and
the sea. Topographically Lokkarfjord has very steep walls rising from the sea level to plateau c. 600
m higher up. Lokkarfjord is not mapped in detail, but observations made in the visit, supported by
samples collected by Often and Schiellerup (2008), indicate the rock type on the sea level to be
magnetite enriched ultramafic hornblendite while the plateau level is found to be composed of
coarse grained mafic hornblende gabbro. The chemistry of the Lokkarfjord deviates substantially
1 km
1 km
gn MZ gb
MZ
umaf
umaf
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 5
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
from all other Seiland intrusions as having high phosphorus content throughout as described later in
the report.
Fig. 4. Bedrock (circles) and boulder (triangles) observation points and Reinfjord target areas on surface conductivity map. Lakes indicated by white. Day1,… refer to corresponding day descriptions in the text.
Day 1, area 1
Day 1, area 2
Day 1, area 3
Day 2
Day 3
Day 4
Day 5
Day 7
Day 9
Småvatna
Bonjikdalen
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 6
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 5. Geological map of area 1 of day 1. Points R1001-R1011 refer to sampling points. Layering of olivine cumulate (oC) is 090/20. Xe, gabbro xenolith (R1005) 15 m in diameter.
3.3. Tappeluft Roberts (2007) describes Tappeluft Complex (Fig. 12) to comprises coeval pegmatitic gabbro,
ultramafic rock and syenite, intruded into a larger mass of clinopyroxene gabbro. The pegmatitic
gabbro is emplaced as both concordant sheets and discordant dykes and pipes. The ultramafic
portion of the complex comprises clinopyroxenites and peridotites. This deviates bit from what was
visually observed on outcrops, see Day 6 in Chapter ‘Field observations’.
4. Field observations This Chapter describes geological observation on day-to-day basis and discusses shortly on the
implications referring also to assay results and petrophysical properties of rock samples. The field
programme emphasized abundant sampling, totally 106 samples were collected. In addition to that,
a bulk sample of c. 3 kg was taken from Småvatna mineralization for possible concentration tests.
The numbering protocol of samples was based on target area and sampler:
C1001… for samler Iljina,
C1…for sampler Ahvenjärvi, in which
C stands for Target area: R, Reinfjord; L, Lokkarfjord; T, Tappeluft
Samples with coordinates and descriptions are listed in App. 2.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 7
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Physical properties measured and calculated by the Geological Survey of Finland include (App. 3):
-density
-susceptibility
-remanence
-calculated Q-ratio
-resistivity measured by galvanic method using three different frequencies (0.1, 10, and 500 Hz)
-conductivity measured by inductive method
-calculated chargeability 1 and 2
In text it is referred to geophysical instrument called Proxan. Proxan is a portable EM device
designed to measure conductivity of bigger boulders and bedrock down to about 4 m, 8 m in max.
High susceptibility of the rock hampers Proxan measurements precluding detection of weaker
conductors though the good conductors would be detected despite of high magnetite content.
Samples collected from the Reinfjord intrusion are depicted on geological map of Fig. 2 and surface
conductivity map of Fig. 4.
The airborne geophysical results referred in this Chapter refer to interim results and interpretations
provided by SkyTEM before the field work session. Later Nordic Mining contracted Revelation
Geoscience Ltd to perform interpretations on the airborne final results.
Day 1, Aug. 16th
, miscellaneous subtarget areas
Area 1. Stratigraphic sample profile starting from garnet gneiss in the west, passing through
marginal zone (c. 20 m thick) and variable olivine cumulates (oC) and ending to Langstrand gabbro
in the east (Fig. 5). This profile was made as MIGC team had a helicopter in use and to visit this
remote area would have been impossible in the short time available for NTNU student team, which
otherwise was in charge of geological mapping. Also, according to available mapping data, the site
had most of the Reinfjord rock types exposed in a small area enabling stratigraphic sampling. 11
samples collected, R1001-R1011.
Observations and conclusions: Reinfjord ultramafic complex has the width of about 600 m on
present erosion surface. The Marginal Zone in contact with the garnet gneiss, is well
developed and has rather sharp contacts. This MZ is weathered and crumbles readily in
sampling. The mineral composition was interpreted ultramafic, plagioclase bearing
pyroxenite. MZ has rusty colour, but no visible sulphides were detected. The olivine cumulate
(oC) of the layered series is well-layered and has large pyroxene oikocrysts. Contact between
olivine cumulate and Langstrand gabbro is of ‘interlayered’ type in which oC and gabbro
‘layers’ follow each other on the surface profile.
Area 2. Field check of airborne conductivity anomaly (Fig. 4). An area of 150 m by 70 m was
checked in the centre of the anomaly. Four outcrop samples, R1-R4.
Observations and conclusions: Few sulphide grains were encountered in a gabbro looking
enclave (3m*6m) in olivine cumulate. The amount sulphides encountered do not explain
conductivity anomaly. The 3D interpretation of airborne conductivity measurement indicates
conductor to dip SE and extend to depth of c. 300 m referring that it is not related to surface
weathering phenomena. The reason for conductivity anomaly remains unconfirmed, but an
interpretation, that it is caused by sulphide precipitation triggered by assimilation of gabbro
slabs, can be put forward. Much more sulphides than encountered on surface are, however,
needed to explain conductivity anomaly.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 8
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Area 3. Field check of airborne conductivity anomaly, which plots over the Langstrand gabbro (Figs
2 and 4). Two mineralized gabbro boulders and one unmineralized outcrop sampled, R5-R7.
Observations and conclusions: The outcropped bedrock on the lake shore is unmineralized
banded gabbro. The topography rises steeply to SW from the lake and several fallen sulphide
mineralized gabbro boulders were found. Sulphide occurred in bands (layers?), which may
easily lead rock to be a galvanic conductor. Further supporting evidence comes from the
observation made in the following day (Aug. 17th
), when a thick (0.5 m) sulphide bearing
layer in gabbro gave positive reading in Proxan measurement.
Day 2, Aug. 17th
, ‘The Lake District’ Area of lowered resistivity locates in the centre of the ultramafic complex and no reason for
lowered resistivity was known. The conductive body has also depth extension. In contrary, the
known sulphide dissemination of the marginal zone in eastern edge of the conductive area did look
not to show up in the conductivity map. The Lake District is also a magnetic low. 18 samples
collected R1012-R1018, R1053, R1054, and R8-R15 (Figs 6 and 7).
Observations and conclusions: Field check gave no field indications for the lowered
resistivity. Only few sulphide grains were encountered in the oC in the centre of the anomaly.
Due to lower susceptibility of the Lake District the Proxan survey was possible. Proxan
indicated weak (up to 15 units), but undisputable conductivity anomaly in the vicinity of the
sampling points R1013 and R1053 (Fig. 6). Due to limitations of Proxan device, the
conductor should be in depth of less than 10 m.
The Langstrand gabbro has sulphide bearing layers 2-50 cm in thickness. The thickest layer
gave conductivity signal when measured by Proxan. The Contact Zone between oC and
Langstrand gabbro was interlayered and the slabs of gabbro into Reinfjord ultramafics were
rather sizeable i.e. maybe few tens of meters thick and few hundred of meters long. The
NTNU students have distinguished pyroxenite (Marginal Zone proper) and crossover zone
(i.e. that interlayered zone) in the Contact Zone (Fig. 7). Lake District marginal zone was
observed to resemble Småvatna and Bonjikdalen in terms of amount of sulphides and
continuity of mineralisation.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 9
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 6. Lake District, sampling points on the conductivity map of depth interval 10-15 m, SkyTEM interim results. Lakes and rivers outlined. Circles are outcrop and triangles are boulder observations. Sampling site R1013-R1053 shows the conductor recognised by Proxan.
Fig. 7. Lake District, sampling points on the geological map. Lakes and rivers outlined. Circles are outcrop and triangles are boulder observations.
0 250 500
Meters
!.
!.
!.
!.
!.!. !.
!.
!.
!.
!.
#*
!.
!.!.!.!.
!.
!.!.
524770
524770
524970
524970
525170
525170
525370
525370
525570
525570
525770
525770
525970
525970
526170
526170
526370
526370
77
76
54
377
76
64
3 77
76
74
377
76
84
3 77
76
94
377
77
04
3 77
77
14
377
77
24
3 77
77
34
377
77
44
3 77
77
54
377
77
64
3 77
77
74
3
0 250 500
Meters
Dunite Peridotite
Olivine pyroxenite
Pyroxenite
Crossover zone Sulphide mineralised
Langstrand gabbro
R1013 R1053
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 10
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Day 3, Aug. 18th
, The Valley
A 1.7 km long east-west oriented conductivity anomaly runs to east of lake Storvannet (Elljajávri).
The area is also magnetic low. The anomaly follows a rather deep valley, which has been
interpreted to follow a fault zone, along which the northern block has moved eastwards about 200
m. A sample profile was taken along the olivine cumulates of valley complemented by two
Marginal Zone samples (Figs 8 and 9). Twelve samples collected R1019-R1026 and R16-R19.
Observations and conclusion: Clear evidences of the fault zone was found as the olivine
cumulates were sheared and a vertical banding (cm wide bands) had been developed
paralleling the strike of the valley. The true magmatic layering was yet still visible and dipped
gently to SSE (135/30). One striking observation was that the rocks were distinctly magnetic
in field measurements and the laboratory measurements indicated one of the highest
susceptibility values for the ‘Valley’ samples (up to 150 mSI units) in Reinfjord intrusion
(Fig. 10). This contradicts to magnetic low in the SkyTEM results. Reason to that is most
likely that there are magnetic rock masses (valley walls) above the measuring magnetometer.
No sulphide grains were detected in the olivine cumulates, but in the eastern end of the profile
cavities after sulphide weathering (mm size) and possible silicate replacement of sulphide
grains (pyrite crystal shape) were anticipated. (Assay results revealed however, one sample to
contain some sulphides.) The porosity is also expressed by low resistivity readings in galvanic
conductivity measurements. The ‘Valley’ samples form also a group of their own in
susceptibility vs. density plot (Fig. 10) as being characterised by high susceptibility and low
density. Lowered density and resistivity may both originate from shearing.
In the western end of profile the Valley cuts the Marginal Zone. MZ outcropping on south
side was mapped to be sulphide bearing by Söyland Hansen (1971). These sulphides were
verified by local sulphide bearing pyroxenite boulders found in this field trip. Local boulders
also indicated the MZ on northern side of the fault to be sulphide bearing as well (R1025).
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 11
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 8. The Valley, sampling points on the magnetic maps. Lakes and rivers outlined. Circles are outcrop and triangles are boulder observations.
Fig. 9. The Valley, sampling points on the conductivity map of depth interval 10-15 m. Lakes and rivers outlined. Circles are outcrop and triangles are boulder observations.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 12
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 10. Susceptibility [µSI] vs. density [kg/m3] of all samples. The Valley olivine cumulate samples highlighted by
blue-green. Lokkarfjord samples circled.
Day 4, Aug. 19th
, Småvatna mineralization
An about 20 m thick and 2 km long sulphide mineralization has been reported by Söyland Hansen
(1971) between Bonjikdalen and Småvatna the latter locating in the northern end of the zone.
Geologically it is located close (in few tens of m) or at the lower contact of the Reinfjord intrusion
against garnet gneiss (Fig. 2). The reported (NGU) nickel and copper values are presented in the
Table 1. PGE values were reported to be negligible (on few ppb level) by NGU. Bonjikdalen-
Småvatna zone did not show up in standard processing of SkyTEM data or in detailed work made
by contract geophysicist.
TABLE 1. REPORTED (NGU) NI, CU, AND S CONTENTS OF SMÅVATNA AND BONJIKDALEN. TABLE
ALSO PRESENTS NI AND CU CONCENTRATIONS ALLOTTED TO 100% SULPHIDES (MSF).
Valley
Density
3 4503 4003 3503 3003 2503 2003 1503 1003 0503 0002 9502 9002 8502 8002 7502 7002 6502 600
Su
sc
1 000
10 000
100 000
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 13
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
The stratigraphic position, thickness, and mode of sulphides make Bonjikdalen-Småvatna deposit as
a typical representative of Contact Type Ni-Cu-PGE deposit though PGE was low. A sample
traverse and some erratic samples were collected, R1027-R1041. In addition, a bulk sample of c 3
kg was taken (smaller rock chips representing the traverse).
Observations and conclusion: The chemistry of Småvatna samples is discussed in more detail
in Chapter ‘Whole-rock Chemistry’. All samples with only few exceptions were rather
weathered and the sulphide content as well as the relative metal ratios in the sulphide fraction
are possibly not initial. Visually the total amount of sulphides corresponds to those reported
by NGU.
Day 5, Aug. 20th
, Airborne conductivity anomaly
The aims of this visit were to study a weak airborne conductivity anomaly about 1 km to NW from
the Lake District and the Marginal Zone further to NW (Figs 2 and 4). Six samples taken, R1042-
R1046, and R20.
Observations and conclusions: No explanation whatsoever was found for the conductivity
anomaly. However, reasonable amount of sulphides was found in the Marginal Zone
pyroxenite (often pegmatitic) right underneath the olivine cumulate of the layered series.
These sulphides formed dm size pockets (R1042, Table 2) while rest of the MZ was less
mineralized. An interlayered type relationship between Langstrand gabbro, pyroxenite and
maybe also including some layered series, as found in the Lake District, was noted here also.
Evidences of assimilation of country rock (Langstrand gabbro in this case) into the magma
resulting in varitextured rock were documented here (Fig. 11).
Fig. 11. Varitextured gabbro in a marginal zone, close to sample sites R1042-R1046, Day 5.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 14
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Day 6, Aug. 22nd
, Tappeluft
Tappeluft is about 3.5*1 km2 complex (Fig. 12) comprising of coeval pegmatitic gabbro, ultramafic
rock and syenite, intruded into a larger mass of clinopyroxene gabbro. Scattered observations of
pentlandite and other sulphides are made in Roberts’ thesis (2007). Observations came from the
ultramafic part as well as from the gabbropegmatite. Whole-rock analytical data indicated however
very low Ni values for all of those samples. Totally eight samples were taken, T1001-T1007, and
T1.
Observations and conclusion: Contrary to earlier descriptions on Tappeluft as a
clinopyroxenite-dunite intrusion, visual observations in the field refer to amphibole rich rock.
Field observations also confirmed Tappeluft intrusion to contain some sulphides up to weak
dissemination towards to NE contact (arrow in the Fig. 12), the sulphide bearing traverse
along the road was c. 350 m. An erratic sulphide occurrence was also found closer to SW
contact of the intrusion. Two samples were also taken from the sea shore, one better
mineralized gabbropegmatite boulder sample and one less sulphide mineralized coarse
grained gabbro outcrop sample. Field observations also referred to an younger generation of
gabbropegmatite (Fig. 13).
Fig. 12. Sampling sites on Tappelulft intrusion, map after Roberts 2007. The arrow indicates sulphide bearing traverse along the road side (samples T1001-T1005). Sample T1 represents an erratic sulphide occurrence, while T1006 (boulder) and T1007 are sulphide mineralized coarse grained pegmatitic gabbros.
T1
T1001-T1005
T1007
T1006
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 15
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 13. Gabbropegmatite close to the sea shore in Tappeluft.
Day 7, Aug. 23rd
, Bonjikdalen mineralization
Reader is asked to check day 4 (Aug. 19th
) report for background information. A sample profile of
six samples was made, R1047-R1052. The collection of bulk sample for concentration tests was left
to be done by NTNU students.
Observations and conclusion: The chemistry of Bonjikdalen samples is discussed in more
detail in the Chapter ‘Whole-rock Chemistry’. Bonjikdalen traverse turned out to be much
fresher compared to Småvatna in the northern end of the zone. These samples should
represent initial sulphide content and metal ratios in the sulphide fraction.
Day 8, Aug. 24th
, The Lake District The Lake District was revisited, now together with the Norwegian team. The reader is asked to
check the description of the day 2 (Aug. 17th
).
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 16
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Day 9, Aug. 25th
, weak conductors on Northeast Marginal Zone
Aim of this visit was to study the Northeast Marginal Zone, encountered weak conductivity
anomalies, and gabbro xenoliths in the NEMZ. Northeast Marginal Zone represents the least
explored part of the Reinfjord intrusion and more of it has been exposed due to withdrawal of
Langfjordjøkelen glacier. Two boulder samples, R1055-R1056.
Observations and conclusion: The contact zone between NEMZ and the Langstrand gabbro
was observed to be similar as in the Lake District i.e. interlayered and containing gabbro
slabs. The NEMZ was also found sulphide bearing; one sampled boulder was composed of
pyroxenite with patches of plagioclase bearing olivine cumulate (troctolite).
Day 10, Aug. 26th
, Lokkarfjord Lokkarfjord is rather small (c. 2 km
2) ultramafic-mafic intrusion surrounded by younger gabbro and
the sea. Two massive sulphide dykes had been documented from Lokkarfjord close to the sea shore
in steep mountain wall. Both had been verified to have high Ni and Cu (0.5-1% Ni and Cu, max
2.2% Ni and 4.5% Cu, Vrålstad 1977), while the other one was also assayed for PGE (0.8 ppm
Pt+Pd, Often and Schiellerup 2008). Norsk Hydro had made two 400 m long VLF measurement
profiles over the dykes, measurements had not revealed other dykes in the vicinity of the mapped
dykes. Detailed processing of SkyTEM conductivity data reveals also these dykes. Purpose of the
visit was to resamples the dykes and get updated conception of the dykes. In addition to that, the
aim was also to do Proxan survey on the Lokkarfjord plateau to see if more dykes are present higher
up in the topography and stratigraphy. Topographically Lokkarfjord has very steep walls to sea and
a plateau c. 600 m above the sea level. 22 samples were taken, L1001-L1014 and L1-L8.
Observations and conclusions: In order to get general distribution of the sulphides, a sample
profile was taken along the lowermost exposed bedrock outcrops (Fig. 14). Fifteen samples in
total, was taken from that traverse of about 110 m in lenght. The lowermost exposed rocks
were hornblendites. The fabric of the rock is vertical and obviously also the sulphide bodies
have vertical elongations. -In addition to sample profile, several rusty boulders on the sea
shore were sampled.
Many of the very rusty boulders actually turned out to have only little visible sulphides, but
were enriched in magnetite. The relative abundance of sulphides and magnetite varied a lot
and was unable to be judged on the weathered rock surface. The high magnetite content could
be seen in the susceptibility values, which were 100-400 mSI units. Lokkarfjord samples are
also forming a group of their own in susceptibility vs. density plot (high susceptibility and
high density, Fig. 10) due to magnetite and pyrrhotite content.
Due to steep topography, and high and variable susceptibility of the hornblendite, Proxan
study was not possible. However, on the plateau level the rock type was mafic hornblende
gabbro with lower susceptibility enabling Proxan survey, which, however, didn’t reveal any
surface conductors. The texture of that gabbro gave an impression to the author, that it
represents evolved, late stage crystallisation product.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 17
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 14. Sample profile over Lokkarfjord sulphide dykes. Lok 41- Lok 43 refer to sampling of Often and Schiellerup (2008).
5. Whole-rock chemistry All 106 samples collected during the field trip were subjected to chemical assays performed by ALS
Chemex laboratories. Precious metals Au, Pd, and Pt were assayed by ICP after lead fire-assay
preconcentration (PGM-ICP23), while rest of the 33 elements of the assay package ME-ICP61 were
assayed by ICP-AES after near total four acid leach. Over one weight percent of Ni and Cu
concentrations were assayed by Ni-OG62 and Cu-OG62 methods, respectively. Above counted
assay methods are accredited.
L1004 L1006
L1007
L1008 L1009
L2 L3
L7
L1013
L8
L1012
L1011 34 m L6 74 m L1010 90 m
L1005
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 18
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
In order to get better estimates for the composition of sulphide fraction 39 samples were chosen to
sulphide specific assays utilising L-ascorbic acid / hydrogen peroxide solution (ME-ICP09). Nickel,
copper, and cobalt are assayed by ICP-AES from the solution. Two samples with high sulphur
content (>10% S) were assayed by Leco (S-IR08) to get accurate whole-rock sulphur contents for
those.
5.1. Quality assessment ALS Chemex had used in-house standards, duplicates, and blanks to control the quality of the
assays. For the reason that ALS Chemex sulphide specific assay method is not accredited the
following quality test was made. Due to mineralogy of copper, all Cu is assumed to be bound to
sulphides and the total (Cut) and sulphide specific (Cusp) assay results for copper should be the
same. The calculated relative percentage difference (RPD) averaged to 3.4% with three assay pair
exceeding RPD 10% (Fig. 15). In over half of the sample pairs sulphide specific gave slightly
higher reading, but only up to 5%. The quality of the sulphide specific assays can be interpreted to
fulfil requirements for studies discussed in this report. For sample pairs with Cut>>Cusp a
mineralogical study is warranted to check the copper mineralogy.
Fig. 15. Relative percentage difference between total copper and sulphide specific copper analyses. Positive value denotes total concentration higher than sulphide specific and vice versa.
5.2. Theoretical background Definition of the terms used in the discussion:
Sulphidic metal content, Msp The amount of metal bound in sulphide minerals and therefore
amenable to recovery in sulphide flotation
Silicate metal content The amount of metal bound in silicate minerals
Total metal content, Mwr The amount of metal in the rock
Metal concentration in
sulphide fraction, Msf
The amount of metal in the 100% sulphides
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 19
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Following modal sulphide mineral assemblages were assumed for the basis of Msf calculations:
Reinfjord,
modal proportion
Lokkarfjord,
modal proportion
S content of
mineral, wt%
Pyrrhotite 67 % 55 % 38.0
Chalcopyrite 15 % 15 % 35.0
Pentlandite 3 % 15 % 33.0
Brovoite 12 % 0 % 53.0
Pyrite 3 % 15 % 53.5
Weighted S content
of 100% sulphides 39.7 39.6
Despite of differing sulphide mineral composition Reinfjord and Lokkarfjord sulphide assemblages
have about the same amount of sulphur i.e. 40% S in 100% sulphides; this value was used in
calculations of sulphide fraction compositions.
Distribution coefficient (D) describes the partitioning of an element between sulphide and silicate
melt. For base metals like Cu and Ni as well precious metals, D is in favour to sulphide melt. D for
copper is inorder of 250-1,000 i.e. copper content of sulphide melt in equilibrium with the silicate
melt is 250-1,000 times higher than the associated silicate melt. D for nickel is dependent on the
MgO content of the magma and values 180-200 can be applied for magmas forming the Reinfjord,
for example. D for PGE is very high, in order of 10,000-100,000. Discussion handles also term
called R factor, which by definition is mass ratio of silicate melt to sulphide melt. The metal
contents of the very first sulphides can be calculated simply by using the partitioning coefficient but
when more sulphide melt is formed, the silicate melt gets depleted in metals and hence metal
concentrations in the sulphide melt is decreasing.
R factor can be calculated using the formula (1):
R= (XiDi-YiDi)/(Yi-XiDi), in which (1)
Xi, content of metal i in the silicate melt,
Yi, content of metal i in the sulphide melt, and
Di, distribution coefficient of metal i.
Because DPd >> DCu any withdrawal of sulphide melt would leave the residue silicate melt with
higher Cu/Pd ratio. Mantle derived melts are assumed to have Cu/Pd ratio in order of about 4,000-
20,000, the upper bound being for olivine tholeiites. Early sulphides after sulphide immiscibility
have Cu/Pd ratio closer to that of magma and any later formed sulphides have lower ratio, while the
silicate residue enriches in Cu relative to Pd.
For the reason that the formula (1) presumes knowledge of initial concentrations of metals prior to
sulphide melt separation, which is seldom adequately known, rocks Cu/Pd can be used to
approximate the R factor (App. 1). This method utilizes different D values of Cu and Pd, and
development of Cu/Pd ratio as a function of R factor.
5.3. Småvatna and Bonjikdalen sulphide chemistry Representative assay results of the Småvatna and Bonjikdalen samples are presented in the Table 2.
Samples collected in this field trip formed profiles over the mineralised section and results should
objectively present metal concentration in the section.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 20
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
One striking feature is the very low precious metal values. The bit higher PGE contents of olivine
cumulate of Layered and Central Series (R8, R16, and R1053) highlight Småvatna and Bonjikdalen
low precious metals contents. Cu/Pd ratio is extremely high, often 100,000-500,000, which also
points relative depletion of Pd.
Unlike the precious metals, the base metals Cu and Ni seem to be concentrated in the amounts
typical to Contact Type magmatic sulphides. Figure 16A shows Ni concentrations in 100%
sulphides to vary generally between 3-4 wt% while that of copper shows larger scatter as varying 3-
5 wt%. Total amount of sulphides in the rock has no effect on base metal concentrations in 100%
sulphides as shown in the Fig. 16A. The amount of silicate bound nickel in the marginal zone can
be estimated to c. 180 ppm (Fig. 17).
The calculated Cu and Ni values in 100% sulphides in Reinfjord MZ are also in line with
concentration tests presented by Söyland Hansen (1971), who reported values of 5 wt% Cu and 4
wt% Ni in sulphide concentrate.
Figure 16C shows that the Langstrand gabbro has much lower tenor of base metals in sulphide
fraction than the Reinfjord marginal zone.
Approximation of R factor is presented in App. 1. Low PGE and relatively high base metals in the
sulphide fraction refer to R factor (formula 1) of about 1,000, which together with very high initial
Cu/Pd ratio may have resulted in metal ratios present in marginal zones (see also cautionary
statement in App. 1). The study also suggests prior enrichment of Cu in the silicate melt up to level
of about 200-250 ppm. External Cu may have been brought to the system by assimilation of
Langsrtrand gabbro (see Table 2).
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 21
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
TABLE 2. REINFJORD. TOTAL AND SULPHIDE SPECIFIC ASSAY RESULTS, AND CALCULATED
CONCENTRATIONS IN 100% SULPHIDES OF SELECTED ELEMENTS. PEAK VALUES IN BOLD.
Cu Cu Ni Ni Ni Co Co S Au Pt Pd PGE+Au
Assay type SP SF WR SP SF SP SF WR WR WR WR SF
Sample site ppm wt% ppm ppm wt% ppm ppm wt% ppb ppb ppb ppm
Marginal Zone
R1029 Små 880 4.19 727 590 2.81 70 3333 0.84 6 7 5 0.86
R1030 Små 400 3.64 578 370 3.36 30 2727 0.44 3 <5 2 -
R1031 Små 1120 5.89 839 740 3.89 60 3158 0.76 6 12 12 1.58
R1035 Små 350 4.67 250 120 1.60 20 2667 0.30 3 <5 3 -
R1039 Små 710 4.44 756 500 3.13 40 2500 0.64 3 10 <1 -
R1048 Bon 1240 5.06 1130 970 3.96 60 2449 0.98 2 <5 3 -
R1049 Bon 340 3.58 573 400 4.21 30 3158 0.38 1 14 <1 -
R1050 Bon 590 3.06 860 650 3.38 50 2597 0.77 1 8 2 0.57
R13 LD 450 2.47 692 580 3.18 40 2192 0.73 3 31 1 1.92
R14 LD 770 2.08 1335 1280 3.46 90 2432 1.48 2 6 3 0.30
R15 LD 620 2.61 974 890 3.75 60 2526 0.95 3 <5 1 -
R1015 LD 510 2.10 1070 920 3.79 50 2062 0.97 2 22 <1 -
R1016 LD 800 2.27 1470 1370 3.89 100 2837 1.41 4 8 5 0.48
R1054 LD 840 3.54 807 650 2.74 70 2947 0.95 11 5 5 0.88
R1025 Stor 320 3.46 660 480 5.19 40 4324 0.37 <1 9 <1 -
R1042 Day 5 260 3.47 542 330 4.40 40 5333 0.30 1 <5 1 -
R1056 NEMZ 1630 4.08 3640 2970 7.43 170 4250 1.60 12 26 33 1.78
R3 Nwing 1870 19.18 1620 1140 11.69 70 7179 0.39 47 14 1 6.36
Langstrand gabbro
R1017 LD 200 0.71 220 220 0.78 40 1416 1.13 2 <5 2 -
R7 Tverfj 140 0.26 68 70 0.13 60 1116 2.15 1 <5 2 -
R1055 Tverfj 60 0.60 65 60 0.60 50 5000 0.40 1 <5 1 -
Miscellaneous
R8 LD 279* - 1805 - - 146* - 0.17 7 30 26 -
R1053 LD 103* - 2340 - - 156* - 0.07 2 98 37 -
R16 Valley 533* 3690 - - 144* 0.18 219 93 122 -
* total whole-rock concentration Site: Assay type: Små; Småvatna WR; total, whole-rock Bon; Bonjikdalen SP; sulphide specific LD; Lake District SF; calculated concentration in 100% sulphides Stor; Storvannet (Elljajávri) NEMZ; Northeast Marginal Zone Nwing; North wing of Reinfjord intrusion Tverfj; Tverfjordalenvann (Jiehkkejávri) Valley; valley to east of Storvannet (Elljajávri)
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 22
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 16. Copper and nickel in 100% sulphides (Msf) versus whole-rock sulphur. Some strongly deviating samples excluded.
Småvatna and Bonjikdalen
Rest of Reinfjord MZ
Langstrand gabbro
S, wt%
Msf, wt%
S, wt%
Msf, wt%
S, wt%
Msf, wt%
A
B
C
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 23
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 17. Total whole-rock Ni (Niwr) versus sulphidic Ni of Småvatna and Bonjikdalen samples.
5.4. Scattered observations from Reinfjord intrusion The marginal zone in the Lake District (Table 2, Fig. 16B) gave similar base and precious metal
readings as the Småvatna and Bonjikdalen. Observations outside of these three areas are scarce but
areally small sulphide enriched pockets were found. Two samples (R1056 and R3) representing
pyroxenitic Northeast Marginal Zone and the conductive area studied in Day 1/Area 2, stand out
with metal contents higher than Småvatna-Bonjikdalen-Lake District MZ.
It is worth of note that one sulphide mineralised sample of olivine cumulate of the Central Series
from the eastern end the Valley profile (Day 3, R16) had the highest gold reading from all 106
samples assayed i.e. exceeding the contents of Lokkarfjord massive sulphides. This Valley sample
(R16) had 219 ppb Au (1,800 ppm S). Gold enrichment can be related to shearing.
5.5. Genesis of Reinfjord sulphides The position of Reinfjord marginal zone hosted sulphides is typical for many layered intrusions.
Features of wallrock assimilation and mixing of melts on intrusion margins refer to dynamic
intrusion event. These characteristics and especially the sulphide content of contaminant,
Langstrand gabbro, may well have resulted in sulphide saturation and precipitation of marginal zone
sulphides. The Cu and Ni concentrations in 100% sulphides are on typical level for many Contact
Type deposits. The precious metal concentrations are, however, very low. The precious metal data
of the olivine cumulates of the layered series is limited, but some samples taken have PGE
concentrations higher than the sulphide enriched marginal zone samples. While the structural
position and base metal chemistry points strongly to orthomagmatic sulphides, the low precious
metal concentrations call for additional explanations. Following models can be proposed:
Magma was depleted in PGE due earlier withdrawal of sulphides
Magma was depleted in PGE initially due to processes in the mantle
Additional Cu and Ni, but no PGE, was introduced to magma by local contamination. This
together with low R factor (possibly lower than approximated in App. 1) gave rise ‘normal’
base metal concentrations but negligible PGE.
In summary, the MZ sulphide chemistry is not in ‘balance’ to what would be expected to have
formed from Reinfjord type silicate melt. Metal ratios may also have been affected by pervasive
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 24
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
fluid activity, which reworked metal ratios of the sulphide melt rendering R factor calculations
inadequate, for example.
5.6 Lokkarfjord sulphide chemistry The samples profile of fifteen samples (Fig. 14) failed to locate massive sulphides. However, the
whole profile is rather constantly sulphide bearing up to 2.7 wt% S (Table 3). The composition of
Lokkarfjord sulphide fraction is highly variable (Fig. 18). Some samples having whole-rock sulphur
content between 0.5-1.0 % S have less than one weight percent of Ni and Cu in 100% sulphides. On
the other hand some massive sulphide samples have decent Ni and Cu contents between 2-5 % of
both metals. Ni/Cu ratio is variable most samples being however copper dominated (Table 3).
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 25
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
TABLE 3. LOKKARFJORD. TOTAL AND SULPHIDE SPECIFIC ASSAYS, AND CALCULATED
CONCENTRATIONS IN 100% SULPHIDES OF SELECTED ELEMENTS. PEAK VALUES IN BOLD. O, OUTCROP
SAMPLE AND B, BOULDER SAMPLE.
Cu Cu Ni Ni Ni Co Co S Au Pt Pd PGE+Au
Assay type SP SF WR SP SF SP SF WR WR WR WR SF
Sample O/B ppm wt% ppm ppm wt% ppm ppm Wt% ppb ppb ppb ppm
Profile
L1004 O 120 0.94 78 50 0.39 30 2353 0.51 <1 <5 1 -
L1005 O 120 1.04 66 40 0.35 30 2609 0.46 1 <5 2 -
L1006 O 360 3.27 100 80 0.73 50 4545 0.44 2 <5 3 -
L1007 O - - 116 - - - 0.14 <1 <5 <1 -
L1008 O - - 7 - - - 0.09 1 <5 <1 -
L1009 O 70 0.85 16 <10 - 10 1212 0.33 1 <5 1 -
L2 O - - 44 - - - 0.25 1 <5 2 -
L3 O - - 31 - - - 0.28 2 <5 1 -
L8 O 750 5.56 715 460 3.41 40 2963 0.54 7 12 47 4.89
L1013 O - - 299 - - - - 0.15 1 <5 3 -
L7 O 1160 3.22 1240 1020 2.83 80 2222 1.44 12 27 100 3.86
L1012 O 4330 6.46 2010 1680 2.51 150 2239 2.68 16 34 149 2.97
L1011 O 80 1.07 <1 <10 - 10 1333 0.30 1 <5 <1 -
L6 O 150 0.79 6 10 0.05 50 2632 0.76 3 5 <1 -
L1010 O - - <1 - - - - 0.08 1 <5 <1 -
Miscellaneous L1 B 15850 5.33 5520 5440 1.83 470 1580 11.9 159 142 1005 4.39
L4 B 1330 3.83 1205 970 2.79 80 2302 1.39 16 29 107 4.37
L5 O 140 0.86 20 20 0.12 40 2462 0.65 3 <5 4 -
L1001 B 1340 3.06 1325 1160 2.65 90 2057 1.75 18 26 123 3.82
L1002 B 1440 4.24 1135 960 2.82 80 2353 1.36 14 24 92 3.82
L1003 B 10000 3.20 12000 11900 3.81 1120 3584 12.5 105 183 637 2.96
L1014 B 220 2.26 26 20 0.21 40 4103 0.39 <1 <5 <1 -
Assay type: WR; total, whole-rock SP; sulphide specific SF; calculated concentration in 100% sulphides
The base metal concentrations in Lokkarfjord sulphide fraction (Fig. 18) are generally slightly
lower than in the Reinfjord (Figs 16A-B). There is also no correlation between whole-rock sulphur
content and copper and nickel concentration in 100% sulphides as the two almost massive sulphide
samples (L1 and L1003) have similar Cusf and Nisf than the disseminated samples. Lokkarfjord
precious metal concentrations are about double to those of Reinfjord (in 100% sulphides). The R
factor study presented in App. 1 refers to about one decade higher R factor (R ~5,000-10,000) for
Lokkarfjord than for Reinfjord.
It is noteworthy that nine of 22 collected samples had phosphorus content over one weight percent.
These results are parallel with the results received by NGU (Often and Schiellerup 2008), who
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 26
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
reported P2O5 contents of 1-3 wt%, and not only for the hornblendites of the shore line but also to
hornblende gabbros of Lokkarfjord plateau. No mineralogical study to explain these chemical
characteristics is available.
Fig. 18. Copper and nickel in 100% sulphides (Msf) versus whole-rock sulphur.
5.7. Tappeluft sulphide chemistry In line with the field observations, Tappeluft samples are sulphide bearing S varying 400-3,700
ppm. Copper contents were 21-149 ppm and nickel 210-487 ppm. Precious metal concentrations are
below or at the detection limits.
6. Conclusions
6.1. Reinfjord
6.1.1. Geophysical survey
The interpretation of the helicopter survey on the Lake District was performed by Revelation
Geoscience Ltd (Johnson 2011). Two conductors were modelled, one shallow and one deeper the
latter locating little bit to the east from the shollower one (Fig. 19, and Tables 4 and 5). The upper
contact of the shallower conductor is modelled to depth of only 50 m while the deeper has the upper
contact at the depth of 205 m. The modelled conductance of 50 Siemens is low and is not referred to
massive sulphides.
TABLE 4. MODEL PARAMETERS OF THE WESTERN CONDUCTOR AFTER JOHNSON 2011.
Easting (centre of top edge) 525405 mE
Northing (centre of top edge) 7777165 mN
Elevation (centre of top edge) 550 m
Dip 13°
Dip Direction 126°
Plunge 0°
Strike length 600 m
Down‐dip extent 125 m
Conductance 48.4 S
S, wt%
Msf, wt% Lokkarfjord
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 27
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
TABLE 5. MODEL PARAMETERS OF THE EASTERN CONDUCTOR AFTER JOHNSON 2011.
Easting (centre of top edge) 525690 mE
Northing (centre of top edge) 7777160 mN
Elevation (centre of top edge) 450 m
Dip 8°
Dip Direction 126°
Plunge 0°
Strike length 600 m
Down‐dip extent 300 m
Conductance 50 S
Fig. 19. Surface projection of the conductors modelled in Lake District (Johnson 2011). Stippled line indicates the gabbro screen, which noted to be sulphide bearing in the eastern end (Söyland Hansen 1971). Circle indicates the recognised Proxan conductor.
The other conductors worth of mentioning are those of so-called Valley conductor (Day 3, Fig. 4)
and one in the north wing of the Reinfjord intrusion (Day 1, Area 2). The layer inversions produced
by SkyTEM Surveys indicates the latter conductor to dip to SE to depth of c. 300 m at the angle of
40-45 degrees. Both conductors are however too small or their resistivity still too high for
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 28
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
modelling. The same features may be applicable to explain why Småvatna-Bonjikdalen and other
marginal zone mineralization show up so poorly.
The Fig. 20 depicts susceptibility versus Q-ratio with discrimination fields for various
ferromagnetic mineral compositions. In that diagram Reinfjord samples plot to fine-grained
magnetite field and differ from those of Lokkarfjord.
Fig. 20. Susceptibility [µSI units] versus Q-ratio of Reinfjord () and Lokkarfjord () data. Discrimination fields are based on GTK database (Airo 2005).
6.1.2. Geological interpretation and ore genesis
Our field observations confirmed the high quality of old mappings of Söyland Hansen (1971) and
Emblin (1985) in terms of lithology and accuracy of geological maps.
The MZ was found sulphide mineralized practically every places where visited. Excluding
Småvatna, Bonjikdalen, and Lake District, the amount of sulphides varied from few erratic grains to
weak dissemination and small sulphide pockets. Visually better than average sulphide contents were
detected in the MZ at the eastern Lake District, on the top of the mountain between the Lake
District and Lake Storvannet (Day 5) and in a pyroxenite of Northeast MZ (Day 9). The Layered
Series and Central Series were found unmineralized except few erratic sulphide grains.
The garnet gneiss and Langstrand gabbro surrounding the ultramafic intrusion were found sulphide
bearing, an observation was also made that certain thicker sulphide bands contained enough
sulphides to be conductors (Day 2) and some airborne conductivity anomalies can be caused by
these sulphide bands (Day 1, Area 3).
The following suggestion for geological interpretation of the conductivity anomalies of the Lake
District is based on intimate spatial relationship of gabbro slabs and sulphides. The Småvatna-
Bonjikdalen zone locates under the giant gabbro slab, though not immediately, but separated by a
slice olivine cumulate of LS layer (Fig. 2). Småvatna and Bonjikdalen are typical representatives of
Contact Type sulphide deposits found in contact zones of many layered intrusions. The genesis of
Contact Type deposits is often attributed to country rock contamination. To form immiscible
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 29
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
sulphide melt, the incorporation of external sulphur into magma is especially required in Reinfjord
due to high initial Mg content of the magma; high Mg magmas have high capability to dissolve
sulphur. The sulphide content of garnet gneiss underneath the deposits, though not well studied,
looks negligible, but Langstrand gabbro carries reasonable amounts of sulphides in many places
thus providing the only documented source for external sulphur. Field evidences refer to model, in
which the Lake District conductors are sulphides originated due contamination caused by the
Langstrand gabbro. Proposed cross-section showing the field relationship of ultramafic intrusion,
marginal zone and gabbro is depicted in Fig. 21.
Fig. 21. Geological model for the conductors (cross-hatched) modelled in the Lake District. gn, garnet gneiss; gb, Langstrand Gabbro; MZ, Marginal Zone; umaf, ultramafic units.
A more far going model can also be postulated. The Lake District locates close the southern tail of
the Central Series, which may have acted as a feeder for the main mass of CS. One can put forward
a model in which CS magma intruded through the mineralized Contact Type deposit and reworked
and enhanced the mineralization. However, the high nickel content (1,800-2,500 ppm) of the
olivine cumulates locating right above the conductors indicate that these rock have not experienced
any voluminous sulphide withdrawal in their history. Also, the olivine cumulate (R8 and R1053)
over the modelled conductors show higher PGE contents than any marginal zone samples.
6.1.3. Recommendations
Modelling gave low conductivity values (about 50 Siemens, Tables 4 and 5) for the conductors in
the Lake District. The two extreme models to result in such conductivity values are (i) cm-dm thick
bands of interconnected sulphides and (ii) thicker heavily disseminated layer or body of sulphides.
Both models are supported by the field findings. By reference to observations made on Day 2,
thicker sulphide bands in the Langstrand gabbro give conductivity signal. On the other hand, the
marginal zone with its gabbro slabs and xenoliths host tens of meters thick disseminated sulphides.
In economic point of view the latter model with heavily disseminated sulphides is more positive due
to reason that the sulphides encountered in the MZ are of acceptable quality in terms of their Ni and
Cu content in the sulphide fraction and the metal concentrations stay the same with increasing total
amount of sulphides (Figs 16A-B). More massive concentrations of these sulphides would be
potential for economic deposit.
Due to reason, that the conductors do not outcrop, drilling is the only mean to get hard evidence
from the conductors. In order to get more precise 3D concept of the conductors and to direct the
drilling, ground geophysical survey is necessary to be undertaken. A TEM method is recommended.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 30
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
6.2. Lokkarfjord Lokkarfjord is unconventional type massive Ni-Cu-PGE deposit. Lokkarfjord sulphides carry
higher PGE concentrations than those found in Reinfjord. The closest analogy is the N-K-T
discordant sulphide veins in the 2.5 Ga old Monchegorsk layered intrusion in Kola Peninsula (see
more Mitrofanov et al. 1997 and Iljina 2011). N-K-T was a remarkable nickel mine and it exploited
(closed in 1970’ies) a swarm of vertical sulphide veins, which had considerable continuity in terms
of strike length and depth extension. These veins were narrow, the thickest being only 50 cm. A
viable genetic model for Monchegosk veins is that they represent dilatational cracks formed during
magma cooling and consolidation. These cracks localized low viscosity interstitial immiscible
sulphide liquid present in the consolidating cumulus pile.
6.2.1. Geological interpretation and ore genesis
Lithologically Lokkarfjord intrusion is composed of ultramafic hornblendite at the sea level, but the
Lokkarfjord plateau 600 m higher up is coarse grained mafic hornblende gabbro. A modified
Monchegorsk model can be suggested to Lokkarfjord. Instead of extensive veins, sulphide pods
were formed in Lokkarfjord. Individual pods may have vertical long axis, but are less developed
horizontally.
6.2.2. Recommendations
Metal characteristics of the Lokkarfjord sulphides is presented in the Fig. 18. Nickel and copper
contents in 100% sulphides are variable, but attaining the level of several weight percent. In the
case of massive sulphides, the threshold of tonnages for mining is distinctly lower than for much
lower grade Reinfjord Contact Type deposits though both have similar Ni and Cu concentrations in
100% sulphides. Careful examination of airborne geophysical data revealed four weak conductors
(Fig. 22) distributed on the shore line, one of these (conductor A, Fig. 22) coincides to sulphide
dykes studied in this field trip. The steep topography and flight line orientation prohibit further
utilization of SkyTEM measurements. Suitable conditions for the formation of the pods may only
have been in the ultramafic lower part of the magma chamber. If so, a swarm of sulphide pods may
well have formed. For this reason and also because Lokkarfjord is the only known locality for more
PGE enriched sulphides in SIP, further exploration is recommended. More work may also produce
key observations, which can be used for exploration in other Lokkarfjord type intrusions in SIP.
Due to hundreds meters high steep wall of the intrusion, the exploration and verification of the
possible pod swarm is a great challenge. Though the known sulphide bodies were visible in
SkyTEM survey, the survey is incapable to detect sulphide bodies inside the mountain. One way to
approach is to do suitable geophysical ground survey, like Max-Min (Slingram) along the sea shore.
Possibilities to make a loop for TEM measurements on the steep wall should also be examined.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 31
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Fig. 22. Weak conductor indications (A-D) in Lokkarfjord. Red triangle indicates the site of known sulphide
dykes.
6.3. Tappeluft Large portion of profile along the road across the intrusion (Fig. 12) was noted to be sulphide
bearing up to weak disseminations. Sulphides are, however, low in base metals and especially low
in precious metals. Gabbropegmatites on the shore line were similarly low in metals concerned.
Wide distribution and lack of any obvious controlling feature for the sulphide distribution refer that
the minor precipitation of iron sulphides occurred along with the silicate crystallisation i.e. magma
was at sulphide saturation. No accumulation of sulphides to form more massive bodies or sulphides
with higher base metal contents can be forecasted and further exploration cannot be recommended
at the moment.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 32
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
7. Evaluation of the Seiland Igneous Province to host Ni-Cu-PGE
sulphide deposits This Chapter evaluates the Seiland Igneous Province (SIP) to host Ni-Cu-PGE sulphide deposits
making special reference to Reinfjord intrusion. The evaluation is done by making an attempt to
quantify factors critical in ore formation processes. The following factors are surveyed:
-Geotectonic setting, age and character of magmas,
-Sulphide saturation,
-Encountered deposits and mineralisation indications
Evaluation is done by comparing typical features of igneous complexes hosting Ni-Cu-PGE
deposits to those documented from SIP. Seiland data is collected from Emblin (1985), Robins 1996,
Roberts (2007), and Larsen (2011) and combined with observations made in the fieldwork
described in this report.
7.1. Geotectonic setting, age, and character of magmas
SIP consists mafic and ultramafic plutons emplaced into a sedimentary succession indicative for a
continental setting. The plutons are relatively small in area, but are numerous, with more than ten
discrete mafic plutons and five large ultramafic bodies having been identified. Significant volumes
of intermediate monzonitic and dioritic rocks, as well as nepheline syenite and carbonatitic intrusive
material do accompany mafic and ultramafic magmatism. Alkaline rocks are present in both
discrete complexes and dykes, and are generally crosscutting mafic plutons. Of the total 5,500 km2
areal extent 50% comprises mafic gabbros and 25% ultramafic intrusions, which are composed of
peridotites (lherzolites, wehrlites), dunites, pyroxenites, and hornblendites.
Reinfjord ultramafic intrusion has been interpreted to have formed by two subsequent intrusion of
ultramafic magma the former producing olivine and pyroxene bearing cumulates and the latter
mainly olivine cumulates, dunites.
SIP was emplaced and crystallized in a short time span of about 10 Ma 560-570 Ma ago.
Volumetrically largest mafic and ultramafic intrusions are aged to be formed in even shorter time
span of only 4 Ma. The Province is interpreted to have extensional setting, possibly in an
intracontinental rift or in a back-arc setting.
Geotectonic setting
Most of world’s major PGE occurrences are hosted by intracontinental rift related layered
intrusions. These intrusions are also known for their Cr and Fe-Ti-V oxide deposits, but lesser
extent for their Ni-Cu deposits.
Geotectonic setting of SIP is strongly favouring PGE mineralization.
Magma compositions
The large variety of magmas present in the Province points to heterogeneity in the source area and
to differentiation processes during the ascent of magmas with possible auxiliary magma chambers
at lower levels. Emblin (1985) did estimate the Ni content of the magma in response of the
Reinfjord intrusion to have been between 240 and 490 ppm. Values over 400 ppm are characteristic
for komatiitic magmas, which are typical hosts for many nickel deposits. However, the Ni assays of
SIP rocks, as presented by Roberts (2007), show low Ni content of the olivine cumulates (<<1,000
ppm). Compared to these low values, the Reinfjord intrusion stands out for its higher Ni content
(order of 1,000-3,000 ppm), which resemble olivine cumulates of many komatiites.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 33
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
The prevailing pyroxene in SIP mafic and ultramafic intrusions is clinopyroxene. This is in contrast
to majority of other intracontinental intrusions, where the prevailing pyroxene is orthopyroxene.
This orthopyroxene dominance has been attributed to siliceous high-Mg basalt nature of the
magmas, which are thought to have high initial PGE content.
Diversity of magmas and high Ni content of some of them are strongly favouring Ni mineralization,
especially in Reinfjord.
Domination of clinopyroxene over orthopyroxene is suggesting deviating magma compositions
between SIP and most of world’s PGE mineralized intracontinental layered complexes.
Age
Globally Paleoproterozoic and Archean deposits are dominating hosts for PGE deposits while
nickel deposits are more evenly distributed over the geological time (Fig. 23).
Young age of SIP is not supportive for PGE mineralization.
Fig. 23. Quantitative distribution of PGE (above) and Ni (below) resources over the geological time after Maier and Groves, 2010. Age scale in Ga.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 34
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
7.2. Sulphide saturation Mafic magmas are more capable to dissolve sulphur than more siliceous magmas due to lower
polymerisation and vacant positions available for sulphur atoms in the structure of magma; the
ultramafic magmas have of course the highest sulphur carrying capability. In general, the sulphur
content of mafic magmas is well below the capability of magma to dissolve it. In order to form
sulphidic Ni-Cu-PGE ore, the sulphur dissolving capacity of magma should be exceeded. Factors
driving magma towards to sulphur saturation are decreasing temperature, increasing oxidation
degree, and increasing polymerisation. In natural systems the most common factor for increasing
polymerisation is the addition of silica, aluminium, and ferric iron into the magma. On the other
hand, decreasing pressure increases sulphur solubility. Finally, the fastest way to reach the sulphur
saturation is the addition of external sulphur into the magma. In practise all Contact Type Ni-Cu-
PGE deposits hosted by mafic-ultramafic complexes have been attributed to wallrock
contamination. Most common contaminants are sulphur bearing siliceous and aluminous rocks like
black shales and other sulphurous sediments. In the case of ultramafic magma, a gabbroic
contaminant lowers magma’s sulphur solubility due its higher aluminium and silica contents. In
addition to in-situ wallrock contamination, some processes related to evolvement of magma during
the ascent and interaction between magma pulses may have resulted in high grade Ni-Cu-PGE
deposits in rare cases (Iljina and Lee, 2005). No indications of such processes in Reinfjord or
elsewhere were observed in this study.
Reinfjord intrusion is the only one in SIP being in contact with sedimentary country rocks (garnet
gneiss). Småvatna-Bonjikdalen zone is in contact to these rocks. Contact zones of Reinfjord
intrusion to sulphide bearing Langstrand gabbro are also sulphide mineralised.
Well-developed layering and fractionation in terms modal and cryptic layering and replenishment
structures are characteristic to all igneous complexes hosting Reef Type deposits though many
intrusions having such features are avoid of PGE mineralisation.
Hasvik Gabbro of SIP has been interpreted to have crystallized under the pressure of 6-8 kbar
meaning the depth of c 25-30 km in the middle crust, which is an applicable crystallisation depth
range for the entire SIP. This is in contrast to most of the intracontinental intrusions, which have
much shallower crystallisation depths.
Availability of external sulphur from Langstrand gabbro and garnet gneiss and evidences of
wallrock assimilation favour Ni-Cu-PGE sulphide formation in Reinfjord.
Well-developed layering and multiple magma injections are in favour of Reef Type PGE deposit in
Reinfjord.
Deep crystallisation depths of SIP intrusions favour formation of immiscible sulphide melt.
7.3. Encountered deposits and mineralisation indications Lokkarfjord massive sulphide bodies and Reinfjord Contact Type deposits are the only documented
deposits in SIP. Other observations of sulphides are limited from microscope observations of
sulphides to preliminary notes of some sulphides hosted in the contact zone of Kjerringfjord
peridotite, Stjernøy Island (Norsk Hydro 1971). Most of the Reinfjord Contact Zone was observed
to be sulphide bearing, but in much lesser extent outside of the Småvatna, Bonjikdalen and Lake
District sections. Though the exploration has been insignificant since 1970´ies, as judged from the
amount of exploration reports available, the number of showings is small making Reinfjord
exceptional within SIP.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 35
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Low number of documented deposits is not supporting SIP to be highly potential for Ni-Cu-PGE
deposits.
Reinfjord and Lokkarfjord intrusions stand out from rest of the SIP as hosting relatively more
sulphide deposits and indications.
7.4. Quantitative evaluation Table 6 quantifies factors favouring and disfavouring Ni-Cu-PGE ore formation potential.
TABLE 6. QUANTITATIVE EVALUATION OF FACTORS FAVOURING AND DISFAVOURING NI-CU-PGE ORE
FORMATION IN SIP IN GENERAL AND REINFJORD IN PARTICULARLY.
Factor SIP Reinfjord Notes
Geotectonic setting ++ ++ + for Ni-Cu / ++ for PGE
Diversity of magmas +++ +++
Pyroxene mineralogy for PGE - -
Age - - Neutral for Ni, -- for PGE
Contamination unknown +++
Igneous textures/structures for PGE +++ +++
Crystallisation depth + +
Number of known deposits -- +
balance
- counts 4 2
+ counts 9 13
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 36
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
8. References
Airo, M-L. 2005. Regional interpretation of aerogeophysical data: extracting compositional and
structural features. In Airo, M.-L. (ed.): Aerogeophysics in Finland 1972–2004: Methods, System
Characteristics and Applications. Geological Survey of Finland, Special Paper 39, 176–197.
Bennett, M., 1971. The Reinfjord ultramafic complex. NGU Bulletin 269, 165-171.
Bennett M., 1974. The emplacement of high temperature peridotite in the Seiland Province of the
Norwegian Caledonides. The Journal of the Geological Society, v. 130/3, 205-228.
Bennett, M., Emblin, S., Robins, B. and Yeo, W.J.A., 1986. High-temperature ultramafic
complex in the North Norwegian Caledonites: I – Regional setting and field relationships. NGU
Bulletin 405, 1-39.
Emblin, S., 1985. The Reinfjord ultramafic complex, Seiland Province: Emplacement history and
magma chamber model. University of Bristol, England, doctoral thesis.
Iljina, M., 2011. Nickel, copper, Platinum-Group Element, and gold potential of Seiland Igneous
Province, Norway. Report for Nordic Mining.
Iljina, M. and Lee, C., 2005. PGE deposits in the marginal series of layered intrusions. in Mungall,
J. (ed.). Exploration for Platinum-Group Element deposits. Mineralogical Association of Canada,
Short Course Series, vol. 34, pp 75-96.
Johnson, D., 2011. Quality assessment and interpretation report on the Reinfjord and Lokkarfjord
SkyTEM surveys. Report for Nordic Mining by Revelation Geoscience Ltd.
Larsen, R., 2011. Ore-forming potential of the Seiland Igneous Province (SIP). Report for Nordic
Mining.
Maier, W. and Groves, D., 2010. Personal communication.
Maier, W. D., Barnes, S-J, DeKlerk, W. J., Teigler, B., and A. A. Mitchell, 1996. Cu/Pd and
Cu/Pt of Silicate Rocks in the Bushveld Complex: Implications for Platinum Group
Element Exploration, Economic Geology Vol 91, pp 1151-1158.
Mitrofanov, F., Torokhov, M. and Iljina, M., 1997. Ore deposits in the Kola Peninsula,
Northwestern Russia. 4th
Biennial SGA Meeting, August 11-13, 1997, Excursion guidebook, B4.
Geological Survey of Finland, guide 45.
Norsk Hydro, 1971. Feltarbeid i Alta-området 1971. Norsk Hydro in-house report.
Often, M. and Schiellerup, H., 2008. Oppfølging av PGE-anomale prøver i Seilandprovinsen,
Finnmark. Report for Nordic Mining, NGU Report 2008.035.
Vrålstad, T., 1977. Svovelberget, Stjernsund, Alta. In-house exploration report of Norsk Hydro.
E X P L O R A T I O N R E P O R T O N R E I N F J O R D , L O K K A R F J O R D , … P a g e | 37
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Roberts, R., 2007. The Seiland Igneous Province, Northern Norway: Age, Provenance, and
Tectonic Significance. University of the Witwatersrand, South Africa, doctoral thesis.
Robins, B. 1996. The Seiland Igneous Province, North Norway. IGCP Project 336, Field
conference and Symposium, Field trip guidebook Part II.
Söyland Hansen, T., 1971. En undersøkelse av nickel-kopper mineraliseringer i Reinfjord-
Jøkkelfjord området, Troms. NTNU Trondheim, M.Sc. Thesis.
List of Appendices:
1 R factor calculations
2 Field observations
3 Petrophysical rock properties.
Rovaniemi December 15th
, 2011.
Markku Iljina
Consulting economic geologist
A P P E N D I X 1 P a g e | 38
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
APPENDIX 1 R factor calculations
R= (XiDi-YiDi)/(Yi-XiDi), in which
Xi, content of metal i in the silicate melt,
Yi, content of metal i in the sulphide melt, and
Di, distribution coefficient of metal i.
Reinfjord
palladium
XPd 1.0 ppb
DPd 10,000
YPd 1.0 ppm
Calculated R factor 1,100
Using this R factor value (1,100) and 4.5 wt% of Cu in 100% sulphides
Reinfjord initial Cu content of the magma XCu =220 ppm.
Lokkarfjord
Lokkarfjord has larger range in palladium values enabling study depicted in Fig. 1. Deduced from that
Lokkarfjord may have had slightly higher R factor compared to Reinfjord. Lower base metals in
Lokkarfjord may be due lower concentration in magma prior sulphide separation.
Fig. 1. Plot of Cu/Pd ratio versus whole-rock Pd in Lokkarfjord. R factor tie lines after Maier et al. 1996.
R=1,000
R=10,000
Cu
/Pd
Pd, ppb
R=100,000
R=100
A P P E N D I X 1 P a g e | 39
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
CAUTIONARY STATEMENT
Above calculations are done by fitting results to account the assay values presented in Tables 2 and 3.
Assay results show large range hampering approximation. Also, R factor calculations are most
effective in the range of 0.1-10*Di and uncertainties are increased close the range limits. The method
also presumes that the formation of immiscible sulphide melt was the only mineralizing process
involved for both base metals and PGE.
The Reinfjord MZ sulphide chemistry is not in ‘balance’ with that what would be expected to have
formed from Reinfjord type silicate melt. Metal ratios may also have been affected by pervasive fluid
activity, which reworked metal ratios of the sulphide melt rendering R factor calculations inadequate.
A P P E N D I X 2 P a g e | 40
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
APPENDIX 2 Field observations Content of Appendix 2
-Table 1, samples with notes
-Table 2, layering observations
-Table 3, susceptibility readings
-Table 4, miscellaneous
TABLE 1. SAMPLES WITH NOTES.
Sample type Easting Northing Notes
Lokkarfjord
L1 BOULDER 559723 7792129 Rusty, bit rounded, sulphides
L2 OUTCROP 559728 7792101 Profile L1004-L1009-L2-L3
L3 OUTCROP 559724 7792102 NW end of Profile L1004-L1009-L2-L3
L4 BOULDER 559721 7792130 Sharp edged, lots of sulph, 1.0*1.0*1.0 cubic m
L5 OUTCROP 559641 7792148 Rusty, but no sulphides
L6 OUTCROP 559641 7792102 Profile L1010-L6-L1011-L1012-L7-L8
L7 OUTCROP 559706 7792067 Some sulphides, Profile L1010-L6-L1011-L1012-L7-L8
L8 OUTCROP 559719 7792066 No sulphides SE end of Profile L1010-L6-L1011-L1012-L7-L8
L1001 BOULDER 559731 7792130 Sharp edged, very rusty, sulphide mineralized 1.5*1.2*0.8 cubic m. Originally formed one big boulder with L1002. Susc. 150 milliSI
L1002 BOULDER 559730 7792129 Very rusty, sulphide mineralized, 1.2*0.6*0.35 cubic m. Originally formed one big boulder with L1001. Susc. 320 milliSI
L1003 BOULDER 559740 7792121 Very rusty, sulphide mineralized, 1.0*1.0*0.6 cubic m.
L1004 OUTCROP 559734 7792082 SE end of Profile L1004-L1009-L2-L3
L1005 OUTCROP 559731 7792084 Profile L1004-L1009-L2-L3
L1006 OUTCROP 559731 7792088 Profile L1004-L1009-L2-L3
L1007 OUTCROP 559729 7792089 Profile L1004-L1009-L2-L3
L1008 OUTCROP 559732 7792098 Profile L1004-L1009-L2-L3
L1009 OUTCROP 559730 7792099 Profile L1004-L1009-L2-L3
L1010 OUTCROP 559624 7792103 Rusty, weathered, NW end of Profile L1010-L6-L1011-L1012-L7-L8
L1011 OUTCROP 559673 7792078 Few sulphide grains, Profile L1010-L6-L1011-L1012-L7-L8
L1012 OUTCROP 559708 7792069 Reasonable sulphide dissemination, Profile L1010-L6-L1011-L1012-L7-L8
L1013 OUTCROP 559714 7792078 No sulphides
L1014 BOULDER 559619 7792165 Very rusty, few sulphide grains visible, oxidized?
Reinfjord
A P P E N D I X 2 P a g e | 41
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
R1 OUTCROP 525721 7780212 Fine-grained umaf
R2 OUTCROP 525662 7780242 Rusty umaf
R3 OUTCROP 525678 7780221 Gabbro enclave, sulphides
R4 OUTCROP 525672 7780219 Gabbro enclave, sulphides
R5 OUTCROP 527717 7778051 Langstrand gabbro
R6 BOULDER 527649 7778005 Sulphide banded Langstrand gabbro
R7 BOULDER 527663 7778016 Sulphide banded Langstrand gabbro
R8 OUTCROP 525368 7777155 oC
R9 OUTCROP 525477 7777123 oC
R10 OUTCROP 525681 7777340 Schistose umaf
R11 OUTCROP 525761 7777172 oC
R12 OUTCROP 526022 7777025 MZ, sulphides
R13 OUTCROP 526112 7776985 MZ, sulphides
R14 OUTCROP 526114 7776988 MZ, sulphides
R15 OUTCROP 526114 7777001 MZ, sulphides
R16 OUTCROP 526051 7778806 oC
R17 OUTCROP 526096 7778802 oC
R18 OUTCROP 526130 7778725 oc
R19 OUTCROP 525586 7778778 oC, schistose, parallel to fault zone
R20 OUTCROP 524754 7777639 oC
R1001 BOULDER 525634 7781543 Fine grained GB, represent bedrock
R1002 OUTCROP 525505 7781616 Poikilitic oC
R1003 OUTCROP 525495 7781602 Poikilitic oC
R1004 OUTCROP 525346 7781550 Poikilitic oC
R1005 OUTCROP 525197 7781535 Gabbro xenolith 15m diam.
R1006 OUTCROP 525194 7781534 Poikilitic oC, coarser
R1007 OUTCROP 525160 7781519 Poikilitic oC, finer grained
R1008 OUTCROP 525068 7781504 Poikilitic oC
R1009 OUTCROP 525021 7781439
R1010 OUTCROP 525025 7781393 Marginal zone, weathered rock
R1011 OUTCROP 525007 7781367 Granulite gneiss
R1012 OUTCROP 525375 7777230 Poikilitic oC
R1013 OUTCROP 525245 7777164 Poikilitic oC
R1014 OUTCROP 525470 7777064 Poikilitic oC, schistose, sulphides
R1015 OUTCROP 526090 7776992 MZ, umaf, weak-moderate sulph. dissem.
R1016 OUTCROP 526101 7776984 MZ, umaf, rusty, oxidized sulphides?
R1017 OUTCROP 526192 7776971 Banded gabbro, rusty band 2-50cm, thickest bands show up by Proxan
R1018 OUTCROP 525664 7777450 Poikilitic oC
R1019 OUTCROP 526127 7778804 Umaf, fine-grained
R1020 OUTCROP 526129 7778820 Umaf
R1021 OUTCROP 526184 7778786 Umaf, possibly few grains of weathered sulphides
A P P E N D I X 2 P a g e | 42
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
R1022 OUTCROP 526183 7778785 Umaf, possibly few grains of weathered sulphides
R1023 OUTCROP 525721 7778769 oC
R1024 OUTCROP 525364 7778863 Well layered oC
R1025 BOULDER 525131 7778974 MZ, pyroxenite pegm 0.5*0.4*0.4 cubic meters, sulphides
R1026 OUTCROP 524917 7778873 MZ, pyroxenite pegm, rusty. Nearby PyPegm boulders sulphide bearing
R1027 OUTCROP 523601 7778377 Småvatna MZ gabbro, moderately sulphides, weathered
R1028 OUTCROP 523630 7778382 Småvatna MZ gabbro, moderately sulphides, weathered
R1029 OUTCROP 523629 7778377 Småvatna MZ gabbro, mederately sulphides, weathered, coarser grained
R1030 OUTCROP 523621 7778381 Småvatna MZ, moderately sulphides
R1031 OUTCROP 523632 7778393 Småvatna MZ gabbro, moderately sulphides, weathered
R1032 OUTCROP 523635 7778407 Småvatna MZ gabbro, moderately sulphides, weathered
R1033 OUTCROP 523636 7778427 Småvatna MZ gabbro, moderately sulphides, weathered
R1034 OUTCROP 523643 7778440 Småvatna MZ gabbro, sulphides, less than lower in the prof, weathered
R1035 OUTCROP 523646 7778452 Småvatna MZ gabbro, little sulphides, weathered
R1036 OUTCROP 523695 7778437 Småvatna MZ gabbro, sulphides, but not necessarily in sample, weathered
R1037 OUTCROP 523671 7778412 Småvatna MZ gabbro, weathered
R1038 OUTCROP 523643 7778375 Småvatna MZ gabbro, little sulphides, fresh
R1039 OUTCROP 523649 7778342 Småvatna MZ gabbro, little to moderately sulphides, weathered
R1040 OUTCROP 523734 7778332 Småvatna MZ
R1041 OUTCROP 523761 7778258 Småvatna MZ gabbro, weathered
R1042 OUTCROP 524670 7778053 MZ, Pyroxenite-Gabbro pegmatite, some sulphides
R1043 OUTCROP 524671 7778048 MZ, Pyroxenite-Gabbro pegmatite right underneath the ULS oC, some sulphides
R1044 OUTCROP 524677 7778097 MZ, not pegmatitic, some sulphides
R1045 OUTCROP 524677 7778054 MZ, rusty PyPegm
R1046 OUTCROP 524795 7777999 MZ, rusty PyPegm, sulphides
R1047 OUTCROP 523813 7777254 Bonjikdalen MZ, lowermost mineralized MZ, fresh
R1048 OUTCROP 523817 7777270 Bonjikdalen MZ, almost net textured sulphides, fresh
R1049 OUTCROP 523829 7777263 Bonjikdalen MZ, almost net textured sulphides, fresh
R1050 OUTCROP 523857 7777260 Bonjikdalen MZ, good sulphide dissem., fresh
R1051 OUTCROP 523865 7777260 Bonjikdalen MZ, less sulphides than lower in the profile
R1052 OUTCROP 523869 7777282 Bonjikdalen MZ, less sulphides than lower in the profile
R1053 OUTCROP 525268 7777158 oC, few sulphide grains
R1054 BOULDER 525950 7777361 MZ, good sulphide dissemination
R1055 BOULDER 527433 7778778 Langstrand gabbro, rusty but no sulphides
R1056 BOULDER 528029 7778823 Pyroxenite with troctolitic patches, some sulphides, 0.6*0.6*0.4 cubic m
Tappeluft
A P P E N D I X 2 P a g e | 43
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
T1 OUTCROP 556923 7777095 Hornblendite, weak-moderately sulphides
T1001 OUTCROP 557303 7777577 Hornblendite, few granis to weak dissemm sulphides, susc. 10-25 milliSI
T1002 OUTCROP 557306 7777593 Hornblendite, few granis to weak dissemm sulphides, susc. 10-25 milliSI
T1003 OUTCROP 557319 7777595 Hornblendite, few sulphide grains, susc. 10-25 milliSI
T1004 OUTCROP 557308 7777643 Hornblendite, weak but even dissem. sulphides, susc. 10-25 milliSI
T1005 OUTCROP 557296 7777636 Hornblendite, increased amount of sulphides, susc. 10-25 milliSI
T1006 BOULDER 555954 7775268 Gabbropegmatite, 0.3*0.15*0.25 cubic m. some sulphide grains. May not be very local boulder
T1007 OUTCROP 555886 7775348 Coarse grained, but not pegm, some oxidized sulphide grains, rusty
TABLE 2. LAYERING OBSERVATIONS.
Reading Easting Northing
1 060/17 525863 7777431
2 060/18 526114 7777001
3 085/20 524699 7777684
4 135/30 525597 7778781
TABLE 3. SUSCEPTIBILITY READINGS.
Reading Easting Northing
30-50 milliSI 525874 7778786
50 milliSI 525943 7778799
50 milliSI 526114 7778783
50 milliSI 526140 7778791
TABLE 4. MISCELLANEOUS OBSERVATIONS.
type code easting northing notes
contact contact between MZ-GB 524633 7778049
contact contact between PyPegm-layered series
524670 7778048
contact contact between R1001-1002 525604 7781567 interlayered contact
contact contact between R1006-1007 525162 7781529
contact contact between R1007-1008 525083 7781508
contact contact between R1010-1011 525022 7781383
other gb slab 527433 7778965 Interlayered NEMZ
A P P E N D I X 2 P a g e | 44
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
other gb slab2 527203 7778901 Interlayered NEMZ
other profile 524600 7781450 mapped from this point to R1001
other profile 557115 7777439 sulphides from this point to NE contact of the intrusion along the road
A P P E N D I X 3 P a g e | 45
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
Appendix 3 Petrohysical properties of the samples TABLE 1. CONDUCTIVITY (INDUCTIVE METHOD), SUSCEPTIBILITY, AND DENSITY MEASUREMENTS FOR
SAMPLES DEPICTED IN THE REPORT TABLES 2 AND 3. GTK ESPOO LABORATORY.
Sample Location or type Conductivity [Siemens/meter]
Susceptibility [10-6 SI] Density [kg/m3]
R1029 Små 48.8 6050 3247
R1030 Små 129.4 7180 3302
R1031 Små 98.0 9100 3198
R1035 Små 198.8 3480 3253
R1039 Små 162.9 2253 3279
R1048 Bon 71.4 11150 3257
R1049 Bon 237.5 14670 3296
R1050 Bon 17.3 9520 3319
R13 LD 237.0 8510 3304
R14 LD 172.7 9910 3326
R15 LD 96.2 4210 3309
R1015 LD 42.2 17150 3377
R1016 LD 42.6 6880 3289
R1054 LD 177.0 8230 3351
R1025 Sto 57.1 25080 3230
R1042 Sto 259.7 35300 3308
R1056 NEMZ 99.0 81500 3044
R3 Nwing 218.3 92700 3046
R1017 LD 33.6 1328 2777
R7 Tverfj 714.3 8520 2936
R1055 Tverfj 515.5 41100 3164
R8 LD 621.1 10620 2970
R1053 Ld 247.5 5570 3364
R16 Valley 100.3 44200 2737
L1004 OUTCROP 806.5 197500 3359
L1005 OUTCROP 840.3 243300 3420
L1006 OUTCROP 2475.2 254000 3378
L1007 OUTCROP 1562.5 225000 3338
L1008 OUTCROP 684.9 286300 3365
L1009 OUTCROP 909.1 211400 3369
L2 OUTCROP 877.2 52100 3253
L3 OUTCROP 813.0 144800 3303
L8 OUTCROP 1253.1 120400 3330
L1013 OUTCROP 259.1 27610 3130
L7 OUTCROP 1150.7 233000 3387
A P P E N D I X 3 P a g e | 46
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
L1012 OUTCROP 211.0 96400 3310
L1011 OUTCROP 3225.8 320000 3480
L6 OUTCROP 4329.0 494000 3471
L1010 OUTCROP 220.3 250500 3359
L1 BOULDER 3610.1 231500 3501
L4 BOULDER 359.7 7060 3336
L5 OUTCROP 684.9 178800 3357
L1001 BOULDER 934.6 161600 3319
L1002 BOULDER 649.4 101500 3279
L1003 BOULDER 237.0 107100 3014
L1014 BOULDER 478.5 148800 3285
TABLE 2. RESISTIVITY (R, CONDUCTIVE METHOD) MEASUREMENTS USING 0.1, 10 AND 500 HZ AC, AND
CALCULATED CHARGEABILITIES. CHARGEABILITY 2 OVER 60% CAN CAUSE AN IP ANOMALY, AND STRONG
ANOMALY IF OVER 70%. GTK ROVANIEMI LABORATORY.
99999=out-of-instrument range
Chargeability 1 = 100 * (R1-R2) / R1
Chargeability 2 = 100 * (R1-R3) / R1
Sample R0.1[Ohmm] R10[Ohmm] R500[Ohmm] Chargeability 1 [%]
Chargeability 2 [%]
R 1001 6610 5930 5120 10.3 22.5
R 1001 7300 6540 5640 10.4 22.7
R 1002 18000 16800 14200 6.7 21.1
R 1003 21000 19400 17100 7.6 18.6
R 1004 79300 71300 62200 10.1 21.6
R 1005 66400 61200 52500 7.8 20.9
R 1006 99999 99999 99999 0.0 0.0
R 1007 27100 25700 24100 5.2 11.1
R 1008 40300 39400 36800 2.2 8.7
R 1009 36800 34700 32500 5.7 11.7
R 1010 21300 20200 18800 5.2 11.7
R 1011 14000 13100 11800 6.4 15.7
R 1012 30000 28500 26500 5.0 11.7
R 1013 25700 24800 23400 3.5 8.9
R 1014 5290 5010 4650 5.3 12.1
R 1015 13300 11200 10100 15.8 24.1
R 1016 372 328 328 11.8 11.8
R 1017 932 923 889 1.0 4.6
R 1018 19000 18400 17100 3.2 10.0
A P P E N D I X 3 P a g e | 47
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
R 1019 561 101 47.5 82.0 91.5
R 1020 336 122 79.3 63.7 76.4
R 1021 272 41.9 25.8 84.6 90.5
R 1022 29700 19500 13700 34.3 53.9
R 1023 597 221 149 63.0 75.0
R 1024 367 131 75.5 64.3 79.4
R 1025 4460 3160 2440 29.1 45.3
R 1026 497 122 82.1 75.5 83.5
R 1027 34800 33200 30800 4.6 11.5
R 1028 30300 27900 24900 7.9 17.8
R 1029 8480 7780 7220 8.3 14.9
R 1030 6480 6110 5640 5.7 13.0
R 1031 567 530 487 6.5 14.1
R 1032 3370 3280 3040 2.7 9.8
R 1033 9520 8690 7460 8.7 21.6
R 1034 13200 12200 11100 7.6 15.9
R 1035 4780 4390 4000 8.2 16.3
R 1036 12200 12100 11600 0.8 4.9
R 1037 17400 16600 15300 4.6 12.1
R 1038 29400 24000 19200 18.4 34.7
R 1039 19500 17700 15400 9.2 21.0
R 1040 4390 4410 4230 -0.5 3.6
R 1041 8100 7770 7290 4.1 10.0
R 1042 3990 3510 3060 12.0 23.3
R 1043 27200 25900 23700 4.8 12.9
R 1043 10400 9830 8810 5.5 15.3
R 1045 837 261 182 68.8 78.3
R 1046 10700 9300 8020 13.1 25.0
R 1047 59000 57100 52000 3.2 11.9
R 1048 5200 4410 3820 15.2 26.5
R 1049 27900 26200 23900 6.1 14.3
R 1050 13400 11800 10200 11.9 23.9
R 1051 34000 32700 29200 3.8 14.1
R 1052 64600 59200 49800 8.4 22.9
R 1053 36600 36900 35800 -0.8 2.2
R 1054 821 700 616 14.7 25.0
R 1055 1790 1150 776 35.8 56.6
R 1056 114 68.7 52 39.7 54.4
R 1 2270 1290 929 43.2 59.1
R 2 1610 730 441 54.7 72.6
R 3 69400 55700 42300 19.7 39.0
A P P E N D I X 3 P a g e | 48
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
R 4 99999 99999 99999 0.0 0.0
R 5 10900 8170 5970 25.0 45.2
R 6 5460 4390 3480 19.6 36.3
R 7 4080 3240 2640 20.6 35.3
R 8 32700 31500 28600 3.7 12.5
R 9 18200 11000 7590 39.6 58.3
R 10 66900 58400 47100 12.7 29.6
R 11 37400 35200 32400 5.9 13.4
R 12 46300 45000 42200 2.8 8.9
R 13 6620 6120 5570 7.6 15.9
R 14 1730 1530 1400 11.6 19.1
R 15 3740 3180 3210 15.0 14.2
R 16 1260 989 837 21.5 33.6
R 17 285 58.2 36 79.6 87.4
R 18 1500 800 701 46.7 53.3
R 19 410 173 117 57.8 71.5
R 20 504 172 101 65.9 80.0
L 1 184 132 98.3 28.3 46.6
L 2 1490 1480 1270 0.7 14.8
L 3 8260 6580 5100 20.3 38.3
L 4 3690 2950 2540 20.1 31.2
L 5 1940 1680 1290 13.4 33.5
L 6 2050 1500 1030 26.8 49.8
L 7 372 137 82.8 63.2 77.7
L 8 4270 3490 2940 18.3 31.1
L 1001 470 292 200 37.9 57.4
L 1002 971 626 459 35.5 52.7
L 1003 240 204 159 15.0 33.8
L 1004 2600 2180 1790 16.2 31.2
L 1005 501 306 247 38.9 50.7
L 1006 1630 1310 1010 19.6 38.0
L 1007 5730 4130 3110 27.9 45.7
L 1008 6660 3910 2580 41.3 61.3
L 1009 4470 2920 2130 34.7 52.3
L 1010 1670 1470 1260 12.0 24.6
L 1011 982 856 786 12.8 20.0
L 1012 367 134 59.1 63.5 83.9
L 1013 11300 11600 11100 -2.7 1.8
L 1014 2280 2170 1770 4.8 22.4
End of Table 2
A P P E N D I X 3 P a g e | 49
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
TABLE 3. CONDUCTIVITY (INDUCTIVE METHOD), SUSCEPTIBILITY AND DENSITY MEASUREMENTS, GTK
ESPOO LABORATORY.
Sample Conductivity [Siemens/meter]
Susceptibility [10-6 SI] Density [kg/m3]
L1 3610 231500 3501
L2 877 52100 3253
L3 813 144800 3303
L4 360 7060 3336
L5 685 178800 3357
L6 4329 494000 3471
L7 1151 233000 3387
L8 1253 120400 3330
L1001 935 161600 3319
L1002 649 101500 3279
L1003 237 107100 3014
L1004 806 197500 3359
L1005 840 243300 3420
L1006 2475 254000 3378
L1007 1563 225000 3338
L1008 685 286300 3365
L1009 909 211400 3369
L1010 220 250500 3359
L1011 3226 320000 3480
L1012 211 96400 3310
L1013 259 27610 3130
L1014 478 148800 3285
R1 357 49700 2902
R2 50 35700 2635
R3 218 92700 3046
R4 88 124800 3001
R5 132 86800 3011
R6 136 11020 3021
R7 714 8520 2936
R8 621 10620 2970
R9 186 29380 2716
R10 68 16240 3012
R11 <10 3770 3320
R12 119 12460 3320
R13 237 8510 3304
R14 173 9910 3326
R15 96 4210 3309
A P P E N D I X 3 P a g e | 50
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
R16 100 44200 2737
R17 72 69100 2624
R18 37 68300 2607
R19 136 93000 2682
R20 89 59000 2901
R1001 108 4290 2848
R1002 149 8440 3300
R1003 46 11210 3299
R1004 98 12570 3291
R1005 155 10600 3174
R1006 29 3760 3258
R1007 30 2077 3252
R1008 95 12980 3251
R1009 254 8810 3238
R1010 65 6000 3120
R1011 27 44600 2672
R1012 79 7310 3375
R1013 248 4720 3389
R1014 150 11990 2819
R1015 42 17150 3377
R1016 43 6880 3289
R1017 34 1328 2777
R1018 79 8140 3293
R1019 345 64700 2614
R1020 <10 133200 2664
R1021 68 103200 2679
R1022 146 7370 3054
R1023 <10 49200 2556
R1024 125 34900 2767
R1025 57 25080 3230
R1026 144 86200 2955
R1027 41 2176 3233
R1028 21 1120 3309
R1029 49 6050 3247
R1030 129 7180 3302
R1031 98 9100 3198
R1032 1475 16430 3250
R1033 1126 12980 3163
R1034 280 16280 3278
R1035 199 3480 3253
R1036 388 1974 3185
A P P E N D I X 3 P a g e | 51
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
R1037 18 865 3191
R1038 65 8680 3334
R1039 163 2253 3279
R1040 45 1704 3259
R1041 606 764 3251
R1042 260 35300 3308
R1043 103 10310 3252
R1044 128 18180 3326
R1045 74 36900 3047
R1046 137 16860 3315
R1047 20 3280 3259
R1048 71 11150 3257
R1049 238 14670 3296
R1050 17 9520 3319
R1051 71 5790 3240
R1052 46 7730 3288
R1053 248 5570 3364
R1054 177 8230 3351
R1055 515 41100 3164
R1056 99 81500 3044
TABLE 4. DENSITY, SUSCEPTIBILITY, AND REMANENCE MEASUREMENTS. Q-RATIO IS
(24.4*SUSCEPTIBILITY)/ REMANENCE. GTK ROVANIEMI LABORATORY.
Density [kg/m3] Susceptibility [10-6 SI]
Remanence [mA/m]
Q-ratio Sample
2860 3080 1210 62 R 1001
3291 8350 5980 34 R 1002
3319 10240 8360 30 R 1003
3300 10940 350 763 R 1004
3214 7740 310 609 R 1005
3282 7430 630 288 R 1006
3264 2030 2170 23 R 1007
3283 12650 3390 91 R 1008
3262 8540 3440 61 R 1009
3044 4090 1260 79 R 1010
2707 48770 5530 215 R 1011
3384 7040 630 273 R 1012
3386 5700 1480 94 R 1013
A P P E N D I X 3 P a g e | 52
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
2814 9330 1720 132 R 1014
3389 17840 4020 108 R 1015
3344 9540 6470 36 R 1016
2768 1110 160 169 R 1017
3290 9200 870 258 R 1018
2632 62760 3330 460 R 1019
2697 156290 11770 324 R 1020
2685 102150 6110 408 R 1021
2972 29930 1580 462 R 1022
2599 53600 2560 511 R 1023
2779 42450 5240 198 R 1024
3280 16830 2690 153 R 1025
2940 77080 6520 288 R 1026
3204 3610 550 160 R 1027
3298 1150 60 468 R 1028
3238 10860 2570 103 R 1029
3311 7230 1230 143 R 1030
3271 4910 1310 91 R 1031
3273 18810 8620 53 R 1032
3201 18340 4160 108 R 1033
3318 25130 4890 125 R 1034
3202 2810 190 361 R 1035
3164 800 40 488 R 1036
3190 900 40 549 R 1037
3330 9130 1930 115 R 1038
3305 2350 260 221 R 1039
3264 1770 60 720 R 1040
3222 990 30 805 R 1041
3332 32390 17210 46 R 1042
3249 14740 5270 68 R 1043
3303 19070 6340 73 R 1044
3013 33600 3130 262 R 1045
3318 16700 8650 47 R 1046
3271 3690 360 250 R 1047
3300 15020 1370 268 R 1048
3322 7040 960 179 R 1049
3306 9210 650 346 R 1050
3257 6350 2830 55 R 1051
3299 8850 770 280 R 1052
3368 5550 1070 127 R 1053
3336 8100 4720 42 R 1054
A P P E N D I X 3 P a g e | 53
Markku Iljina GeoConsulting Tmi Dec 15th, 2011
3152 40370 3270 301 R 1055
3030 73220 4350 411 R 1056
2899 46520 3340 340 R 1
2664 36730 6710 134 R 2
3061 74710 3800 480 R 3
3036 111840 4380 623 R 4
3020 80130 600 3259 R 5
3015 9390 550 417 R 6
2954 7480 620 294 R 7
3005 9530 1180 197 R 8
2751 28620 2200 317 R 9
3010 15040 1120 328 R 10
3326 3720 940 97 R 11
3338 12080 4500 66 R 12
3330 7870 3760 51 R 13
3366 14290 3750 93 R 14
3326 4600 1330 84 R 15
2746 50270 6890 178 R 16
2633 67880 4640 357 R 17
2624 92240 4130 545 R 18
2686 88010 7050 305 R 19
2928 58920 3140 458 R 20
3188 236460 7190 802 L 1
3267 71970 4260 412 L 2
3321 144870 4130 856 L 3
3337 16980 790 524 L 4
3378 203350 10480 473 L 5
3430 392110 18890 506 L 6
3356 180320 5650 779 L 7
3350 132190 5390 598 L 8
3346 124260 3680 824 L 1001
3410 324670 14900 532 L 1002
3206 174960 6050 706 L 1003
3370 237760 5510 1053 L 1004
3458 359890 10480 838 L 1005
3319 241720 4610 1279 L 1006
3323 213980 9390 556 L 1007
3374 267950 9540 685 L 1008
3355 216930 8740 606 L 1009
3349 271980 14970 443 L 1010
3387 339280 11960 692 L 1011
top related