white river property maim block*1 thunder bay miming
TRANSCRIPT
010
GEOLOGICAL MAPPING SURVEYS
conducted on the
WHITE RIVER PROPERTY "MAIM BLOCK*1
THUNDER BAY MIMING DIVISION, ONTARIO
VOLUME I OF II
2.16056NTS: 42C/12
Latitude: 48* 40* N Longitude: 85* 48' W
Owners: Barrick Gold CorporationRoyal Bank Plaza, South Tower, 200 Bay Street, Suite 2700, Toronto, Ontario M5J 2J3
Operator: Placer Done Canada Limited Timmins Exploration Office P.O. Box 960, Timmins, Ontario P4N 7H1
Author: G. Shevchenko (Project Geologist)
Date: May 10, 1995
SUMMARY
The White River Property is located in the Hemlo area of Northern Ontario, and covers the eastward strike extension of the favourable Hemlo stratigraphy.
During the summer of 1994, Placer Dome Canada Limited established 174.7 kilometres of cut line and conducted geological mapping at a scale of 1:2,500. The grid covers a 10km strike extension of the Hemlo package, as well as a 4km strike length of the Gouda Lake Horizon.
The objective of the geological survey was to define the property geology and, in particular, distinguish areas favourable to the development of Hemlo-style mineralization by identifying areas of:
i) felsic porphyry activityii) feldspathic sericitic alterationiii) structural control
The mapped area consists of a northerly dipping package of metasediments and metavolcanic rocks which are sandwiched between the Pukaskwa Gneiss Complex to the south and the Cedar Lake Pluton to the north. The easterly trending Hemlo Fault is interpreted as a northerly dipping, layer sub-parallel, thrust fault and separates the supracrustal rocks into approximately equal east-west trending halves. The northern belt is comprised of clastic metasedimentary and dominantly intermediate metavolcanic rocks, where as the southern belt consists of clastic metasedimentary intercalated with mainly mafic metavolcanic rocks.
The rocks have been metamorphosed to the sillimanite- almandine-orthoclase subfacies of the almandine-amphibolite facies which suggests temperatures and pressures in excess of 6800C and 6kb respectively.
Two phases of ductile deformation (D2 and D3 ) have been observed, and there is no evidence of the D, event within the area mapped. In all cases the supracrustal rocks have a well developed S2 foliation while the St compositional banding is generally restricted to the sedimentary rocks. The S, (crenulation cleavage) is generally most intense proximal to the more competent bodies such as the Cedar Lake Pluton and the Pukaskwa Gneissic Complex.
Within the North Belt, both the S l (compositional banding) and S2 (foliation) dip northward and vary from 320 to 750 and 410 to 72C , respectively. The dips are generally shallower in the southern portion of the belt and steepen in the northern part. The supracrustal rocks are tightly to isoclinally folded about an
IIeasterly trending F2 synformal axis. The axial plane dips northward at 450 to 610 , and the axis plunges westward at 170 to 330 . The plunge is steeper in the western part of the area, and shallows out in the eastern portion. Minor displacements are caused by late, high angle, normal faulting.
Within the South Belt, there is no evidence of a major fold axis, however the rocks do exhibit a strong, easterly trending, penetrative S2 foliation. For the most part, both the S, (compositional banding) and S2 (foliation) dip northward and vary from 060 to 620 and 050 to 700 , respectively. The dips are shallowest proximal to the contact with the Pukaskwa Gneissic Complex. Late, high angle, normal faulting strikes northeast and northwest. Except for the D.C. Lake Fault, where the offset is in the order of 950 metres, displacements are generally minor.
The only evidence of felsic volcanism in the North Belt is the Upper Anomalous Horizon which consists of ash and lapilli tuffs. There is no evidence of hydrothermal alteration adjacent to this unit.
The composition, texture, alteration and rare earth element profile of the Rust Lake Quartz Porphyry is similar to that of the Moose Porphyry. Footwall to the Rust Lake Quartz Porphyry is a garnetiferous sedimentary unit which may represent the metamorphic facies equivalent of argillic hydrothermal alteration.
The East Grid Showing is spatially associated with the main F2 fold axis as well as a deformed body of quartz-feldspar porphyry. This suggests that the fold axis may have been the structure that controlled emplacement of the porphyry and resulting mineralization.
The only evidence of felsic volcanism in the South Belt are the easterly trending Gouda Lake and Thor Lake Horizons. These are considered to be the same and have been offset by the right lateral D.C. Lake Fault. The horizons are sericitic with the intensity of alteration decreasing east of Pickerel Bay and increasing westward from the Thor Lake Showing.
Within the Gouda Lake Horizon, the highest gold grade is restricted to a thin semi-massive sulphide lens at or near the base of the sericitic package. The zone is open at depth and, according to Lac Minerals, has an inferred resource of 167,000 tonnes at 3.51gXt Au, based on 50m polygons. As the drill hole spacing is generally greater than 50m, potential resources may exist in the spaces between.
Near the D3 fold on the east shore of Gouda Lake, the mineralized horizon is very flat lying over a fairly large area and has only been tested by one drill hole. The area north and
Ill
east of this hole is largely untested.
There is evidence of hydrothermal activity along the Thor Lake Horizon, as:
i) a quartz-feldspar porphyry body occurs hangingwall to the massive sulphide showing,
ii) there are local occurrences of garnet and magnetite which may represent metamorphic equivalents of hydrothermal alteration minerals.
As a result of the mapping program, the following recommendations are made:
i) Within the North Belt, the main F2 fold axis may be the structure that controlled emplacement of the felsic porphyry bodies. Exploration should be concentrated along this structure.
ii) The Rust Lake Quartz Porphyry is an attractive Hemlo-type target. Although this was drilled to depth in the immediate vicinity, no previous effort was made to evaluate the porphyry along strike. Further exploration efforts should be concentrated along the strike extension.
iii) Along the Thor Lake Horizon, it appears that thealteration intensity increases in a westward direction. Thus future exploration programs should be concentrated west of White River, and progress towards Frank Lake.
01OCTABLE OF CONTENTS
1.0 Introduction1.1 Location and Access1.2 Physical Environment1.3 Claims and Ownership1.4 History1.5 Summary of Work Performed
2.0 Regional Geology
3.0 Property Geology3.1 Lithologic Descriptions3.2 Structure3.3 Alteration l Mineralization
4.0 Conclusions and Recommendations
5.0 Bibliography
Page
l l 4455
9
12142122
33
36
Table l Table 2 Table 3 Table 4 Table 5
LIST OF TABLESPage
List of Claims Worked 7-9REE Profile - Rust Lake Quartz Porphyry 24REE Profile - Moose Lake Porphyry 25Lithogeochemical Results - East Grid Showing 27Lithogeochemical Results - Thor Lake Showing 32
Appendix I
Appendix II
Appendix III
Appendix IV
Appendix V
Appendix VI
Appendix VII
LIST OF APPENDICES
Statement of Cost
Nature of the East Grid Gossan - R. Lemaitre
Geology of the Gouda Lake Area - R. Lemaitre
Geology of the Thor Lake Area - R. Lemaitre
Progress Report on Ductile Deformation at the White River Property - W.A. Barclay
Lab Analysis Sheets
Statement of Qualifications
LIST OF MAPS
Drawing No.
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General
Property
Title
Location Map
Location Map
Claim Map with Claims (1:40,000)
Grid Location Map (1:
Regional
Property Sheet 'l
Property Sheet '2
Property Sheet '3
Property Sheet '4
Property Sheet '5
Property Sheet *6
Property Sheet *7
Property Sheet '8
Property Sheet (9
Geology
Geology
Geology
Geology
Geology
Geology
Geology
Geology
Geology
Geology
Map
Map
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Worked
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ii
l.O INTRODUCTION
The White River Property is an extensive block of claims that was optioned in 1993 from Lac Minerals Ltd. With the takeover of LAC in the fall of 1994, the ownership of the claims was transferred to Barrick Gold Corporation.
The claims are located just east of the Hemlo gold deposit in north-central Ontario. They cover the eastward strike extension of the Hemlo stratigraphy for a length of some 37 kilometres. The property consists of 888 contiguous claim units, and is arbitrarily divided into two blocks described as follows:
i) Main Block: A rectangular block measuring some 6kilometres wide by 24 kilometres long. It consists of 724 claims and makes up the western two-thirds of the property.
ii) Tail; A long narrow strip measuring some 2 kilometres wide by 13 kilometres long. It consists of 164 claims and comprises the eastern two-thirds of the property.
This report deals with the geological mapping survey that was conducted over a portion of the "Main Block", between June 16th and August 28th (inclusive), 1994.
The objective of the geological survey was to define the property geology and, in particular, distinguish regions that have the potential for hosting Hemlo-style mineralization by identifying areas of:
i) felsic porphyry activityii) feldspathic sericitic alterationiii) structural control
1.1 LOCATION AND ACCESS
The White River Property, which may be found on NTS 42C/11 fi 12, is located in Bomby, Brothers and Laberge Townships, and in the Oskabukuta Lake area of Northern Ontario (Drawings fi and #2). It extends eastward from the Hemlo Mine Site, and is situated within the Thunder Bay Mining Division. The Town of White River is located five kilometres from the eastern-most boundary of the property.
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WHITE RIVER PROPERTY GENERAL LOCATION MAP
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Highway 17 skirts the northern edge of the property and provides access to various portions of the claims by;
i) mineXexploration roads that branch off the main highway across from the David Bell Mine.
ii) boat from White Lake Provincial Park.
1.2 PHYSICAL ENVIRONMENT
Topographically, there are two distinct environments within the mapped area:
i) The area south of White River and west of Pickerel Bay has moderate relief with local steep sections. Elevations vary from 335 to 430 metres, and outcrop exposure ranges from 5 to 203;. Drainage is considered good as the moist, swampy areas are limited and restricted to the valleys.
ii) The area north of White River and east of Pickerel Bay has generally low to moderate relief with elevations ranging from 320 to 420 metres above sea level. Drainage is variable as there are broad areas of low-lying, moist to swampy terrain. Outcrop exposure is generally less than 53;.
The tree types consist of poplar, birch, spruce, jackpine and balsam in the well drained areas, while black spruce and cedar inhabit the low-lying moist regions. The underbrush is generally moderate with local dense patches which consists of alder, moose maple and/or cedar. As a consequence of disease and/or bug kill, 20 to 302; (locally 40 to 503;) of the balsam, jackpine and spruce are dead, resulting in local areas of abundant deadfall.
1.3 CLAIMS AND OWNERSHIP
The claims are 1003; owned by Barrick Gold Corporation (Toronto, Ontario) and are under option to Placer Dome Canada Limited (Vancouver, B.C.).
The White River Property consists of 888 mining claims which may be viewed on Drawing /3.
1.4 HISTORY
As a result of the Hemlo discovery, the "Main Block" of the White River Property was staked in 1980, '81 6 '82. The "Tail 1* portion was staked much later (1989), and was in response to the results obtained in the Gouda Lake area.
Lac Minerals spent 8.1 million dollars on the property between 1981 and 1991 (inclusive). Over the eleven year period, Lac worked the property in a systematic fashion by establishing some 400 line-kilometres of grid and conducting a whole spectrum of surveys on various portions of it. The surveys included geological mapping, magnetometer, IP, CSAMT, mise a la masse, maxi probe, humus geochemistry, trenching, overburden drilling and diamond drilling. Of the total expenditure, some 3.96 million dollars were spent on 30,493 metres of diamond drilling in 145 holes. Most of the diamond drilling was concentrated along the Upper Anomalous and Gouda Lake Horizons.
As a result of the 1991 Supreme Court ruling whereby Lac lost ownership of the Williams Mine, interest in the White River Property waned. Consequently, in 1992 Lac began the process of tendering the property for option.
Placer Dome optioned the property in the fall of 1993, which then totalled 1,264 claims. With what remained of the field season, an airborne radiometric survey was flown and reconnaissance mapping and humus sampling surveys were conducted on a portion of the "Tail". As a result of this exploration program, 364 claims were abandoned in the Tail portion of the property.
In August 1994, American Barrick Resources Corporation was successful in their take-over bid of Lac Minerals, and consequently, ownership of the White River Property was transferred to Barrick. Shortly thereafter, the company changed its name to Barrick Gold Corporation.
1.5 SUMMARY OF WORK PERFORMED
Vytyl Exploration Services (2035 Montrose Place, Thunder Bay, Ontario, P7J 1A4) was contracted for the linecutting. There was a total of 28.7km of cut/surveyed line and 146km cut line that was established (Drawing #4). The baseline trends east/west with cross lines in a north/south orientation. The line spacing is 200m with a station interval of 25m. The stations are identified with pickets and metal tags with the inscribed grid coordinate stapled to them. Although there was a total of 174.7km of line that was established,
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only 133.7km of the grid was covered by the geological survey.
The geological mapping portion of the 1994 exploration program extended from June 16th to August 28th (inclusive). Mapping was conducted at a scale of 1:2,500 along and between the grid lines. Features were located using hip chain and compass as well as GPS (Global Positioning System).
The geological mapping was performed by S. Beauchamp, R. Lemaitre, B. Nelson and G. Shevchenko, with assistance provided by D. Goyette, C. Green, Z. Hunt, A. Mace and M. Sellers. The digitizing and Autocad drafting for this report was carried out by C. Green and C. David. The mapping program was supervised by G. Shevchenko (C/o Placer Dome Canada Limited, Box 960, Timmins, Ontario, P4N 7H1) .
W.A. Barclay Exploration Services Ltd. (23 Grenadier Rd., Toronto, Ontario, M6R iRi) was contracted between June 16th and July 15th (inclusive) to conduct structural mapping and interpretation.
The following table lists the claims and amount of cut line which was actually covered by the geological survey.
Table List of Claims Worked
Claim Number
SSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSM
542588542589542590542591607744607745607746607747607748607749607765607766607767607768607769607770607771607772607787607788
Cut Line (metres)
6501100900650350550650800800800600
120012001200800800800400400750
Claim Number
SSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSM
607789607790607865607866607867607868607869607870607871607872607873607874607878607879607880607881607882607883607884607943
Cut Line (metres)
700 400 nil nil 375 800 800 800 700 900 900 450 300
1500 1300 1650 nil nil nil nil
8
Table fi (cont'd)
Claim number
SSH 607946SSH 607947SSH 607948SSM 607960SSM 607961SSM 607962SSH 607963SSM 607964SSH 607965SSM 607966SSM 607967SSH 607968SSH 607969SSH 607970SSH 607972SSH 607973SSH 625556SSH 625557SSH 625585SSH 625586SSH 625587SSH 625588SSH 625589SSH 625591SSH 625592SSH 625593SSH 625594SSH 625595SSH 625597SSH 625598SSH 625599SSH 625600SSH 625602SSH 625603SSH 625604SSH 625605SSH 625606SSH 625607SSH 625608SSH 625609SSH 625616SSH 625617SSH 625618SSH 625619SSH 625621SSH 625622SSH 625623
Cut Line (metres)
675600nil750 1200 1200800 1500700750900
1000875450800600nilnil 1000 1150300400800800800800800400600800700675400800 1000 1200800 1000 1150 1100800450700225200200800
Claim Number
SSH 625629SSH 625630SSH 625631SSH 625632SSH 625633SSH 625652SSH 625653SSH 625658SSH 625659SSH 625660SSH 625661SSH 625664SSH 625665SSH 625666SSH 625667SSH 625668SSH 625669SSH 625670SSH 625671SSH 625672SSH 625673SSH 625674SSH 625675SSH 625676SSH 625677SSH 625678SSH 625679SSH 625680SSH 625681SSH 625682SSH 625683SSH 625684SSH 625685SSH 625686SSH 625687SSH 625688SSH 625689SSH 625690SSH 625691SSH 625692SSH 625693SSH 625694SSH 625695SSH 625696SSH 625697SSH 625698SSH 625699
Cut Line (metres)
1100250600800nil1325600
112512001050450nil1050
759507007006003504002503256002505508001100120012001200550800900400400800800700700700nilnil750800800800850
a ft (cont'd)
Claim Number
SSM 625700SSM 625701SSM 625702SSM 625704SSM 625705SSM 625706SSM 625707SSM 625708SSM 625709SSM 625710SSM 625711SSM 625712SSM 625713SSM 625714SSM 625715SSM 625716SSM 625717SSM 625718SSM 625719SSM 625720SSM 625721SSM 625730SSM 625788SSM 625789SSM 625790SSM 625791SSM 625792SSM 625793SSM 625794SSM 625795SSM 625796SSM 625797SSM 625798SSM 625799SSM 625800SSM 625801
Cut Line (metres)
400 700 700 800 800 100 800 800 800 800 400 nil 200 300 550 500 500 400 nil 300 200nil800400 1200800 1200 1300400450900400 1050550300700
Claim Number
SSM 625802SSM 625803SSM 625804SSM 625805SSM 625806SSM 625807SSM 625808SSM 625809SSM 625810SSM 625811SSM 625812SSM 625813SSM 625814SSM 625815SSM 625816SSM 625817SSM 625818SSM 625819SSM 625820SSM 625821SSM 625822SSM 625823SSM 625824SSM 625825SSM 625826SSM 625830SSM 625831SSM 625832SSM 625833SSM 625834SSM 625835SSM 626737SSM 626738SSM 1172594TB 1097120TB 1097121
Cut Line (metres)
725 950 900 1150 800 700 1200
50 350 500 500 750 800 400 100 100 150 600 600 400 nil nil 600 750 750 200
1050 1200 1175 650 500 800 800 800 nil 50
2.0 REGIONAL GEOLOGY (Drawing /5)
The White River Property covers part of the eastern extension of the Hemlo Greenstone Belt which is in the Wawa Sub- province of the Superior Province. The belt itself has been subdivided by Muir(1982) into two stratigraphic sequences which appear to be in thrust contact with each other; the Playter Harbour Sequence to the south and, the Heron Bay Sequence to the north.
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The Heron Bay Sequence consists primarily of high iron tholeiitic flows, intermediate to felsic calc-alkaline pyroclastic rocks and related volcaniclastic to epiclastic sedimentary rocks. Burk, et al. (1986) have observed a facies change from coarse pyroclastic rocks in the west, through fine grained pyroclastic and volcaniclastic sedimentary rocks to epiclastic sedimentary rocks in the east.
The Playter Harbour Sequence is characterized by high iron tholeiitic basalt flows and related sedimentary rocks.
Felsic to mafic dykes and sills are locally prevalent, at least some of which may be of subvolcanic origin. Four early Precambrian plutons intrude the supracrustal rocks. The Pukaskwa Gneissic Complex lies to the south and consists mainly of massive to foliated trondhjemite and granodiorite. The Heron Bay and Cedar Lake Plutons are granodioritic in composition and the Gowan Lake Pluton is composed primarily of massive quartz monzonite. Middle to late Precambrian diabase dykes intrude all other rock types.
The supracrustal rocks have been regionally metamorphosed to low grade (greenschist) facies, with local upgrading to medium grade (amphibolite) facies assemblages.
The Hemlo gold deposit is located some 2.5 kilometres from the northwest corner of the White River property. The Hemlo Gold Deposit occurs within highly deformed, schistose, felsic metavolcanic and metasedimentary rocks of the Heron Bay Group. The Hemlo deposit strikes 110 0 to 115", has a continuous strike length of 2.7kms, a known vertical extent of 1.5km, and ranges in width from 3 to 45m (6m average). It exhibits a crescent-shaped geometry, with an average dip of 60 0N, and a plunge of 45 0W.
The deposit is associated with a felsic porphyry intrusive (Noose Lake Porphyry Complex) which is in contact with hydrothermally altered, clastic sedimentary rocks. Specifically, "the ore zones occur as lenses of pervasive microcline alteration distributed within and about the Moose Lake Porphyry Complex" (Johnson et al, 1994). The gold mineralization is associated with disseminated pyrite and molybdenite as well as a complex suite of barium, arsenic, and antimony-rich minerals.
The paragenesis of the deposit has been, and still is, the subject of much debate. Currently, a porphyry-style model is favoured by many workers.
The contained geological reserves at Hemlo are in the order of 80 million tonnes grading 7.7 gramsj tonne gold. The three mines produce 1.3 million ounces of gold yearly, approximately
of Ontario's gold production.
12
3.0 PROPERTY GEOLOGY (Drawings f6 to 14)
The White River Property covers the eastern strike extension of the Hemlo stratigraphy, with the mines located approximately 7 kilometres from the western edge of the area mapped. The geological mapping survey was conducted in the central portion of the property and covers a region measuring some 10 kilometres long (east/west) by 4 kilometres wide (north/south).
The area consists of a northerly dipping package of metasediments and metavolcanic rocks which are sandwiched between the Pukaskwa Gneiss Complex to the south and the Cedar Lake Pluton to the north. The easterly trending Hemlo Fault separates the supracrustal rocks into approximately equal east-west trending halves. The northern belt is comprised of clastic metasedimentary and dominantly intermediate metavolcanic rocks, whereas the southern belt consists of clastic metasedimentary and mainly mafic metavolcanic rocks. According to Muir(1982), the north half would be defined as the Heron Bay Group and the south half the Playter Harbour Group.
The Hemlo Fault has been traced across the property by a combination of mapping and geophysical interpretation. Although the fault itself is not actually exposed, mapping has defined a series of prominent escarpments, while the IP results have outlined a major geophysical break separating laterally continuous belts of high and low resistivity. The Hemlo Fault is interpreted as a northerly dipping layer-sub-parallel thrust fault.
Two phases of ductile deformation have been observed, which, in keeping consistent with T.L. Muir(1993), are the D2 and D, events. There is no evidence of the Dj event within the area mapped. The St is designated as compositional banding which may be the same as the primary bedding (S0 ), while the S2 is the dominant penetrative fabric. In all cases the supracrustal rocks have a well developed S2 foliation while the S, compositional banding is generally restricted to the sedimentary rocks. The Sj occurs as a crenulation cleavage and generally is most intense proximal to more competent bodies such as the Cedar Lake Pluton and the Pukaskwa Gneissic Complex.
For the most part, rocks do not indicate metamorphic grade as the mineralogy (feldspar amphibole biotite quartz) is fairly common throughout the mapped area. However, in the area north of White River, between lines 27000E to 28000E, almandine is stable in the presence of hornblende, biotite and K-feldspar. This defines the sillimanite-almandine-orthoclase subfacies of the almandine-amphibolite facies which suggests temperatures and pressures in excess of 6800C and.6kb respectively.
13
north Belt
The north belt (Heron Bay Sequence) consists of an easterly trending package of intercalated arkosic sedimentary rocks (minor wacke 6 arenite) and intermediate volcanic tuff S flows (minor felsic 6 mafic volcanics). Mafic volcanism is limited and occurs in the south-western portion of the mapped area, just north of the Hemlo Fault (Drawings f6 6 7). Here massive flows and pillowed flows are exposed along the Hemlo Fault escarpment. A single felsic volcanic horizon, previously defined by Lac Minerals as the "Upper Anomalous Horizon, occurs at the northern end of the grid between lines 20900E and 22200E. It is generally narrow (2 to 6m in width), however it does increase to a width of 32 metres (apparent thickness) on line 21400E. It is bounded by intermediate volcanics in the hangingwall and biotite rich arkosic sediments in the footwall.
Both the S] (compositional banding) and S2 (foliation) dip northward and vary from 320 to 75" and 410 to 720 , respectively. The dips are generally shallower in the southern portion of the belt and steepen in the northern part. The supracrustal rocks are tightly to isoclinally folded about an easterly trending F2 synformal axis. The axial plane dips northward at 45" to 610 , and the axis plunges westward at 170 to 330 . The plunge is steeper in the western part of the area, and shallows out in the eastern portion. Minor displacements are caused by late, high angle, normal faulting.
There are several phases of intrusives which cut the supracrustals and have been emplaced at various times during the deformation history. The earliest phases are the quartz feldspar porphyries which appear to have been emplaced prior to D2 . These are only locally exposed, occur as elongated bodies sub-parallel to S2 , and range up to 600m long by 60m wide. The pre-D3 intrusive phases range from diorite to granite in composition and generally occur as bulbous bodies that cut the S2 foliation. These may range in size from ISO by 5Om to 17OO by 300m. The largest is the Cedar Lake Pluton and occurs just north of the gridded area. The diabase dykes represent the latest of the intrusive phases as they were emplaced post D3 . The dykes trend northwest, northeast and north, range up to 50 metres in width and are generally magnetic.
With regards to pre-D2 porphyry activity, of greatest significance are the Rust Lake Quartz Porphyry, located northeast of line 22600E, and East Grid Feldspar Porphyry, situated at 7500N on lines 30000E to 30600E. The Rust Lake Quartz Porphyry is moderately sericitic and hosts up to 33; very fine-grained disseminated pyrite. This porphyry comes very close to being a Moose Porphyry "look-alike". The East Grid Porphyry is unaltered, however it is proximal to the pyritic horizon (East Grid Showing) exposed in the trenches.
14
South Belt
The south belt (Playter Harbour Sequence) also hosts an easterly trending package of rocks, however it consists of a sequence of intercalated arkosic sedimentary rocks (minor wacke 6 arenite) with dominantly mafic volcanic tuffs 6 flows (minor felsic St intermediate volcanics). The supracrustals are bounded to the south by the Pukaskwa Gneissic Complex. The F} recumbent style of folding indicates that the volcanic/sedimentary package was thrust on top of the Pukaskwa.
There is no evidence of a major fold axis, however the rocks do exhibit a strong, easterly trending, penetrative S2 foliation. For the most part, both the S, (compositional banding) and S2 (foliation) dip northward and vary from 60 to 620 and 50 to 7 O0 , respectively. The dips are shallowest proximal to the contact with the Pukaskwa Gneissic Complex. Late high angle normal faulting strikes northeast and northwest, and, except for the D.C. Lake Fault where the offset is in the order of 950 metres, displacements are generally minor.
The only evidence of pre-D2 intrusive activity is the elongated syenite body that occurs just north of White River on lines 25200E and 25400E. As with the north belt, the final phase of intrusive activity is represented by the northeast and northwest trending diabase dykes.
The Gouda Lake and Thor Lake Horizons represent the only evidence of felsic volcanism. These occur in the extreme south portion of the belt and are considered to be the same as they have been offset some 950 metres by the right lateral D.C. Lake Fault. The felsic horizon, which was traced along strike for a distance of some 2.8km, varies in thickness from 2 to 10m with a maximum of 20m at the west end of Gouda Lake. The horizon is characterized by a package of quartz-sericite schist and quartz- eye sericite schist which has a sericite content of 10 to 501;. It is bounded by a thin (0.5-2m) banded wacke in the hangingwall and a 10 to 15m thick wacke/arkosic wacke in the footwall. The alteration intensity decreases east of Pickerel Bay and appears to increase in a westward direction from the Thor Lake Showing. These horizons are discussed in more detail in Appendices III S IV.
3.1 LITHOLOGIC DESCRIPTIONS
Unit 11 Late Mafic Dyke (Diabase)- dark grey to dark greenish grey, weathering to a light
grey to greyish beige- holocrystalline, equigranular, fine to medium-grained and
massive
15
- consists of approximately equal proportions of plagioclase and pyroxene pyrrhotite (up to 33;)
- generally magnetic, and outcrops weather with a rounded appearance
Unit 10 Early Mafic Dike/Sill- dark grey, weathering to a medium grey- equigranular and fine-grained with a well developed
foliation- comprised of approximately equal proportions of amphibole
biotite and plagioclase feldspar
Unit 9 Felsic to Intermediate Intrusive Rocks- generally range from syenite to granite in composition.
Unit 9a Granite- mottled light grey, beige and pinkish grey, weathering
to a light pinkish beige- holocrystalline, hypidiomorphic, generally
equigranular, fine to medium-grained and massive- comprised of quartz (35-45%), feldspar (50-603;) and
biotite(<5%)- may be weakly porphyritic with X-3% potassium feldspar
phenocrysts
Unit 9b Diorite j Granodiorite- mottled grey, white and beige, weathering to a beige
colour- holocrystalline, equigranular, fine to medium-grained
and weakly foliated- consists of plagioclase feldspar (45-60*), potassium
feldspar (S-10%), quartz (<5-20%) and biotite (S-15%) - may also contain l to 31; pyrrhotite or l to 21 magnetite
- may be porphyritic with up to 10* of the feldspar occurring as phenocrysts
Unit 9d Syenite- dark grey with pinkish-orange spots, weathering to a
medium grey with pinkish-beige spots- holocrystalline, equigranular, fine to medium-grained
and massive to weakly foliated- comprised of 85-953; feldspar with 5-153; amphibole
16
Unit 9e Pegmatite Dike- coarse to very coarse-grained feldspar quartz mica- may host two feldspars
Unit 9a Felsic Dike- occurs as a very minor component- very fine to fine-grained- comprised of pink feldspar with 2 to 53; quartz grains
and may have up to 203; amphibole- the selvages may be bleached and appear to be K-spar
flooded- may be deformed and boudinaged
Unit 9h Grey Feldspar Porphyry- mottled light grey and pink, weathering to a light
beige- inequigranular and porphyritic with a weak mineral
foliation- the phenocrysts consist of white potassium feldspar (5
to 203;) ranging from l to 2mm in length- the matrix is fine-grained and consists of feldspar (55
to 753;), quartz (203;) amphibole (up to 53;)- the amphibole may be partially altered to epidote
Unit 9 i Pink Feldspar Porphyry- medium greyish-brown with pink spots- holocrystalline, inequigranular and porphyritic with a
moderately developed foliation- the phenocrysts, which are subhedral, weakly flattened
and rotated sub-parallel to the foliation, consist of 103; pink potassium feldspar (l-4mm)
- the matrix is leucocratic and aphanitic to very fine grained
Unit 9-j Quartz-Feldspar Porphyry- light grey, weathering greyish-white- inequigranular, porphyritic, and weak to moderately
foliated- the phenocrysts consist of white anhedral to subhedral
feldspar (ID-20%) ranging from l-3mm in length and anhedral quartz (S-15%) ranging from 0.5-2mm in diameter
- the matrix is fine-grained and is composed of SO-70% white to grey feldspar and lQ-20% quartz black amphibole (103;)
17
Unit 9k Quartz Porphyry- light grey, weathering greyish-white- inequigranular and porphyritic with a moderately
developed foliation- the phenocrysts (S-15%), which are weakly flattened and
rotated sub-parallel to the foliation, consist of anhedral quartz crystals ranging from 0.5-2mm in diameter
- the matrix is very fine-grained and consists of feldspar and quartz - may have varying degrees of sericite alteration, and may host up to 3% very fine grained disseminated pyrite
Unit 8 Pukaskwa Gneissic Complex- hornblende-biotite bearing tonalite/granodiorite/quartz
diorite- may be plagioclase porphyritic
Unit 7 Arenite- medium grey, weathering medium brown- equigranular and very fine to fine-grained with a weak to
moderate relict detrital texture - may be very weakly foliated
- generally consists of ^0* quartz and <5% mafic with the remainder comprised of feldspar
Unit 6 Arkosic Wacke- generally compositionally banded- less than 50t quartz, less than 153; mafic minerals and
the remainder comprised of feldspar
Unit 6a Feldspar-Ouartz-Biotite Gneiss- light to medium grey, weathering to a medium beige- equigranular, very fine to fine-grained, weakly to
moderately gneissic, and generally compositionally banded
- comprised of 5 to 15t biotite with approximately equal proportions of subhedral feldspar and quartz
Unit 6b Feldspar-Quartz-Biotite-Amphibole Gneiss- banded light and medium grey, weathering to a medium
grey and beige- equigranular, very fine to fine-grained, weakly to
moderately gneissic, and compositionally banded (l-15cm in width)
- the lighter bands consist of subhedral grains of biotite ( 5*) with approximately equal proportions of
18
feldspar and quartz- the darker bands consist of amphibole (5 to 10t) with
approximately equal proportions of feldspar and quartz
Unit 6c Feldspar-Quartz-Amphibole Gneiss- light to medium grey, weathering to a medium beige- equigranular, very fine to fine-grained, weakly
foliated, very competent and may be compositionally banded
- comprised of 5 to 15% amphibole with approximately equal proportions of subhedral feldspar and quartz
Unit 5 Wacke- generally compositionally banded- less than 50% quartz, greater than 15% mafic minerals and
the remainder comprised of feldspar
Unit 5a Biotite-Feldspar-Quartz Gneiss- medium grey, weathering to a light greyish beige- equigranular, very fine to fine-grained, well foliated
and banded- comprised of 15 to 25% biotite with approximately equal
proportions of feldspar and quartz
Unit 5b Biotite-Aaphibole-Feldspar Quartz Gneiss- medium grey, weathering to a light greyish beige- equigranular, fine-grained, moderately foliated and
finely banded with alternate mafic and feldspar rich bands
- consists of amphibole (ID-20%) and biotite (S-15%) with approximately equal proportions of feldspar and quartz
Unit Se Amphibole-Feldspar-Quartz Gneiss- medium grey, weathering to a light greyish beige- equigranular, very fine to fine-grained and weakly
foliated- comprised of 15 to 25% amphibole with approximately
equal proportions of feldspar and quartz
Unit 4 Felsic Volcanic Rocks- banded medium to light grey, weathering beige of rusty
brown- equigranular, very fine to fine-grained with a moderate
to well developed foliation- consists of feldspar (45-65%), quartz ( 20-40*) and
muscovite (lS-20%)- may contain up to 15% disseminated pyrite
19
Unit 4a Felsic Fragmental- medium to light grey weathering light beige- inequigranular, may be compositionally banded, massive
to moderately foliated with a weak to moderate fragmental appearance
- The fragments may consist of either crystal or lithic material. In the case of crystal fragments, they range from l to 3mm in length and consist of anhedral quartz- eyes (<5%) subhedral feldspar ^53;) . In the case of lithic fragments (5-203;), they range from 3 to 15mm and consist of leucocratic material
- The matrix is very fine-grained and consists ofapproximately equal proportions of quartz and feldspar. May contain 2-3% disseminated pyrite and S-10% muscovite laminations.
Unit 3 Intermediate Volcanic Rocks- generally very competent- consists of quartz with 5 to 503; mafic minerals
Unit 3a Massive Tuff/Flow- medium grey, weathering to a dark brown- holocrystalline, equigranular, very fine to fine
grained, weakly foliated and may be compositionally banded
- comprised of amphibole (lfl-15%), biotite (up to 103;), feldspar (40-503;), quartz (35-453;) and may contain 2-43; disseminated pyrite
- flow units may be pillowed
Unit 3b Crystal Tuff- medium grey weathering to a brownish-beige- inequigranular, porphyritic and massive to weakly
foliated- The phenocrysts may consist of either quartz or
feldspar crystals. In the case of quartz they range from 0.5 to 2mm in diameter and constitute up to 53; of the rock. In the case of feldspar they range from l to 4mm in length and constitute up to 103; of the rock.
- The matrix is fine grained and consists of biotite (5- 103;) , quartz (lS-25%) amphibole (^*) with the remainder comprised of feldspar.
- may contain up to 13; disseminated pyrite
Unit 3c Lapilli Tuff- medium to dark grey, weathering to a dark grey and
beige- holocrystalline, inequigranular and foliated with a
20
weak to moderate fragmental textureThe fragments (l to 53;), which may be either monolithicor heterolithic, have been flattened and range inlength from 0.2cm to 5.0cm.The matrix is fine-grained and is comprised ofamphibole (25 to 353;) and feldspar (60 to 701;).
Unit 2 Mafic Volcanic Rocks- no primary quartz and approximately equal proportions of
mafic and plagioclase minerals
Unit 2a Massive Flow- dark grey, weathering medium grey- holocrystalline, equigranular and fine-grained with a
moderate gneissic foliation- comprised of approximately equal proportions of
amphibole and feldspar- may be magnetic
Unit 2b Pillowed Flow- dark grey, weathering medium grey- holocrystalline, equigranular, fine-grained and
moderately gneissic with a distinct pillow texture- the pillows are generally flattened and range from up
to 3m long by 0.4m wide- comprised of approximately equal proportions of
amphibole and feldspar- may be magnetic
Unit 2c Feldspar-Amphibolite- black, equigranular, fine to medium-grained, strongly
foliated and finely banded/laminated with a well developed crenulation segregation cleavage
- consists of black amphibole needles (90-953;) with clusters of feldspar (S-10%)
- the amphibole may occur in radiating crystalaggregates, while the feldspar crystals usually occur in the areas about the strong crenulation hinge - in some areas, the radiating needles cross-cut the foliation and thus may be a thermometamorphic texture.
Unit 2d Quartz-Amphibolite- mottled dark grey and black, weathering to a dark grey- holocrystalline, equigranular and fine-grained with a
moderately developed foliation- comprised of subhedral amphibole (75-853;) and biotite
^53;) with anhedral quartz (ID-15%)
21
Unit 2e Poker Chip Plagioclase Amphibolite- dark grey with beige lenses, weathering grey- essentially equigranular and moderately foliated with a
distinct poker chip fabric- the poker chip texture is caused by lenticular
aggregates (O.5-4Omm long) of fine-grained plagioclase- the matrix consists of coarse amphibole crystals with
finer amphibole and minor plagioclase crystals- the plagioclase portrays varying degrees of
saussuritization- may be variolitic- originally interpreted to be a crystal/lapilli tuff
3.2 STRUCTURE
The complete structural report "Progress Report on the Ductile Deformation at the White River Property" by W.A. Barclay may be found in Appendix V. The following is an excerpt from the principal conclusions section of the report:
"Strain fabrics which are preserved in the region of the White River Property reflect two main ductile deformation events, which may be the latest episodes in a protracted regional tectono-metamorphic history.
Inferred D2 deformation involved intense flattening and development of long-limbed tight to isoclinal folds. Few are discerned within the grid area, but those which have been uncovered are likely parasitic to a major synformal fold closure lying east of Line 28800E at about 8000N. Observed F2 folds are overturned to the north, and characterized by axial planes which lie parallel to an S2 penetrative foliation that is present in almost all lithologies. S2 forms an axial planar fabric to these folds, cutting folded layers in hinge regions at a high angle but trending sub-parallel to F2 fold limbs elsewhere. The limited data obtained thus far suggest that they may have variable plunges in the S2 plane of flattening.
D2 deformation fabrics and transported compositional banding (S,) have been locally overprinted by a D3 crenulation episode. Imprint of this D3 strain has favoured bands and lithologies which are relatively less competent than contiguous units, and/or which have attitudes which are suitable for buckling by N-S shortening along a sub-horizontal axis. A local consequence of D3 strain is that pre-existing D2 fabrics may have been locally reoriented towards S3
22
and towards the shallow alignment of L3 lineations." 1
3.3 ALTERATION/MINERALIZATION
Upper Anomalous Horizon
The Upper Anomalous Horizon, previously defined by Lac Minerals, is a felsic volcanic unit that is situated at the northern end of the grid between lines 20900E and 22200E. It was very much the focus of Lac's exploration program as the majority of the diamond drilling was concentrated along this horizon. Within the mapped area, the unit, which was traced along strike for some 1600m, is generally narrow (2 to 6m in width), however it does increase to a width of 32 metres (apparent thickness) on line 21400E. It is bounded by intermediate volcanics in the hangingwall and biotite rich arkosic sediments in the footwall. The horizon dips northward at 510 to 550 and consists of a package of rhyolitic ash, lapilli and crystal tuffs. Sericite is the main alteration product and it generally occurs pervasively in weak to moderate intensities. There are, however, local intense zones of sericite alteration which occur proximal to the footwall contact. Very fine grained pyrite (2-3%, locally ID-15%) occurs as disseminations and along laminations.
Rust Lake Quartz Porphyry
The Rust Lake Quartz Porphyry was hydraulically stripped by Lac Minerals. The outcrop exposure measures 20 by 65m and is located outside of the grid, some 240m northeast of line 22600E. The porphyry strikes at 2600 to 2S30 and dips northward at 56" to 7O0 . It measures 28 metres apparent width, and was not traced beyond this outcrop. Thehangingwall consists of biotite amphibole bearing arkosic wacke, while the footwall is a garnetiferous biotite wacke. The garnet bearing unit may represent the metamorphic facies equivalent of argillic hydrothermal alteration. The porphyry itself consists of 5 to 103; flattened quartz eyes (up to 2mm long) set in a fine grained felsic matrix that is moderately altered with 15 to 253; pervasive sericite. Pyrite is very fine grained and occurs as disseminations that range from 2-33; and locally 5-103;. Within the porphyry are two 1m wide feldspar porphyry dikes that trend east/west. Both the quartz porphyry and feldspar porphyry
Barclay, W.A. 1994: Ductile Deformation at the White River Property (in house report) j page 18, lines 1-23
23
dykes host a strong F2 foliation that dips 720 in a northerly direction, thus they were emplaced pre-D2 .
The Rust Lake Quartz Porphyry (sample FE06535) and the Noose Porphyry (sample FE06572) were both sampled and run for rare earth elements. Tables 2 6 3, on the following pages, show the results plotted as a rockXchondrite ratio. Although the Moose Porphyry has a marginally higher background in all elements except Lu, the shape and slope of the profiles are very similar. Based on this, as well as textural, compositional and alterational similarities, the Rust Lake Quartz Porphyry comes very close to being a Moose Porphyry "look-alike".
Lac Minerals interpreted the Rust Lake Porphyry as a continuation of the Upper Anomalous Horizon. They tested it with three diamond drill holes and intersected multiple felsic units ranging from 2 to 10m in width. The complete assays were never found (including gold), however the drill summaries show zinc values of up to Q.39%. In drill hole H- 10-2, trace sphalerite occurs over a 73m interval in fractures and veinlets that are hosted in sedimentary and felsic rocks.
East Grid Shoving
Two old trenches were discovered at the very eastern end of the grid. They are located approximately 50m east of Lines 30400E and 30600E, from 7675N to 7875N and 7425N to 7675N, respectively. Both trenches are oriented roughly in a north-south direction and were excavated by Mattagami Lake Mines Limited in the mid-1970's.
The mineralized zone is hosted in a dark grey intermediate volcanic consisting of fine to medium-grained interlocking quartz crystals with minor sericite/muscovite and traces of biotite. The zone, which is bounded on both sides by intermediate volcanics, is proximal to a volcanic7sedimentary contact. It strikes northwesterly, dips 650 ENE, has been traced along strike for 260m and ranges from 9 to 13m true thickness. Mineralization consists of S-5% (often rusted out) pyrite along fractures with traces of a red mineral (cinnabar?) and trace to It molybdenite. "Staining on one sample from the west trench showed up to 103; fine K-spar was present but usually, K-spar was absent. Also present are some unusual grey pods, 10- 50cm in diameter, which contain up to 10% pyrite, abundant stibnite/molybdenite and are very siliceous. These pods do not seem to contain different metals or differ greatly in their concentrations when compared to the rest of the
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26
gossan.
A deformed body of quartz-feldspar porphyry (600m by 60m) has been emplaced near the fold nose, proximal to the eastern trench. The porphyry is "white to tan coloured, medium to fine-grained containing S-10% feldspar phenocrysts and X-2% quartz phenocrysts ranging from O.5-2.5mm in diameter. The matrix is composed of 5% amphibole needles, J.5% quartz, with the rest being feldspar. The unit is weakly foliated and in some places, very strongly folded, consistent with the F2 event." 3
The mineralized zone flanks the main F2 fold axis which has been traced through the entire mapped area.
In the area around both trenches, fourteen samples were sent for analysis, and the results may be viewed in Table 4 on the following page. For the most part, results were disappointing with only one sample (pyritic intermediate volcanic) returning gold above detection limits (ie: 32ppb). "Indicator elements such as As, Sb, and Hg are at or below detection levels. Two of the gossan samples from the east trench, and the three hangingwall pyritic intermediate volcanic lenses in the west trench contained higher than detection level molybdenum."4
The East Grid Showing is discussed in more detail in Appendix II.
Gouda Lake Horizon
The portion of the Gouda Lake Horizon that was mapped is situated at about 5300N and extends from Line 26100E to 1km east of Pickerel Bay. To the east, the favourable horizon continues for several more kilometres, while to the west it is cut by the D.C. Lake Fault and offset some 950m northwest where it becomes the Thor Lake Horizon.
The Gouda Lake Horizon, which was drilled (4200m in 25 holes) by Lac Minerals between 1988 and 1991, has an inferred resource of 167,000 tonnes at S.Slg/t Au.
Lemaitre, R. (1994): Nature of the East Grid Gossan (in house report) j p .2, 1.42 to p.3, 1.4
Lemaitre, R. (1994): Nature of the East Grid Gossan (in house report) j p . 3, 1.15-21
Lemaitre, R. (1994): Nature of the East Grid Gossan (in house report) j p .5, 1.5-8
TABL
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: LI
THO
GEO
CH
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AL R
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TS
- EA
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RID
SHO
WIN
G
Sam
ples T
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Whi
te R
iver
Pro
perty
Sam
ple N
oFE
0620
1FE
0620
2FE
0620
3FE
0620
4FE
0620
6FE
0621
1FE
0621
2FE
0621
3FE
0621
4FE
0621
5FE
0621
6FE
0621
7FE
0621
8 '
FE06
218
Unit -
Loc
ation
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M-F
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MM
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Wes
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Wes
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Wes
tW
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AU •5 5 •5 •5 •6 •6 •5 •S •5 •5 •5 •5 32 •5
AG •5 •5 •5 •S •S •S •5 •5 •6 •6 •5 •5 •5 •5
AS •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2
BA 440
•100 34
077
082
024
076
061
060
062
031
034
025
048
0
BR •1 . . . . . . * . * . * . *
GA3 0 3 3 2 2 2 1 •1 3 4 3 7 3
CO 13 28 6 10 16 90 25 28 16 24 18 81 36 32
CR 66 405 87 46 70 60 34 32 68 60 83 78 440 38
CS 11 4 8 4 6 6 e 6 8 7 e 6 •2 6
FE 2.58
6.66
4.43
2.80
3.86
5.54
6.30
7.40
3.67
7.73
3.75
6.66
6.30
2.66
HF3 2 4 3 6 3 3 3 4 6 4 3 2 3
HO . . . . * •1 •1 * . * . . . .
IR •5 •5 •6 •5 •5 •S •5 •5 •5 •5 •5 •5 •5 •5
MO
270 •5 36 •6 •5 •5 •5 5 •5 e •6 43 12 60
MA34
400
1227
024
200
3320
043
700
3250
016
500
1750
01
3860
028
800
2240
027
200
2080
022
200
Nl •50
•50
•50
•50
•50
•50
160
150
•50
100
100
240
•50
130
RB 77 •30 56 68 38 32 81 38 63 63 55 51 •30 48
SB •0.2
•0.2 0.3
•0.2
•0.2
•0.2
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•0.2
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Sam
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0620
1FE
0620
2FE
0620
3FE
0620
4FE
0620
5FE
0621
1FE
0621
2FE
0621
3FE
0621
4FE
0621
5FE
0621
6FE
0621
7FE
0621
8FE
0621
8
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Wes
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se 11.0
34.0
12.0 7.5
11.0 8.8
6.6
4.8
11.0 8.2
12.0
11.0
35.0 8.7
SE •5 •S •6 •5 •5 •5 •5 •S •6 •5 •6 •5 •5 •5
SN•0
.01•0
.02
•0.01
•0.01
•0.01
•0.01
•0.01
•0.01
•0.01
•0.01
•0.01
•0.01 •0.01
•0.01
SR 0.13
•0.0
5•0
.05
0.15
0.20
•0.0
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07•0
.05
0.1S
0.08
0.12
•0.0
50.
10•0
.05
TA •1 •1 a m . * . . * . . . . *
TH 1.8
4.0
5.6 1.6
6.0
3.5 1.6
1.1 6.6
2.0
4.8
3.8
2.5
2.8
U 1.2
1.8
1.8
•0.6 1.8
0.8
0.8
•0.5
•0.5
•0.5
•0.5 0.8
•0.5 1.2
W •4 •4 •4 •4 •4 •4 •4 •4 •4 •4 •4 •4 •4 •4
ZN 61 156
103
•50
•60 88 68 52 116 88 173
113
116
432
U 11 24 28 12 16 17 11 8 24 14 20 18 16 14
CE 22 60 50 31 37 34 21 21 50 27 37 44 35 31
NO7 25 16 •5 12 13 8 12 24 14 14 18 18 IS
SM 1.3
6.0
2.1 1.5
2.4
2.6 1.7
1.4
4.6
2.4
2.6
3.6
3.6
2.4
EU 0.7 1.6
0.8
0.6 1.1 1.2
0.8
0.7 .8 .1 .2 .4 .4 .2
TB •0.5
•0.6
•0.5
•0.6
•0.6
•0.5
•0.6
•0.6 0.6
0.6
•0.5
•0.5
•0.5 0.6
YB 0.76 1.88
1.02
0.68
0.63
0.73
0.50
0.41 1.23
0.77 1.2
51.0
41.5
60.
82
LU 0.10
0.32
0.17
0.11
0.13
0.12
0.10
0.05
0.20
0.12
0.21
0.15
0.25
0.12
Mas
s28
.28
31.4
627
.87
30.6
025
.64
33.0
038
.36
28.4
531
.12
32.7
430
.74
34.0
430
.50
28.8
1
AU va
lues I
n ppm
exce
pt Au
In pp
b, Ca
, Fa.
Sr, S
n In *
•V
e sign
deno
te be
low de
tectio
n lev
el
28
Generally, the horizon strikes east-west and dips to the north at 210 to 36". It consists "of four distinct subunits; the quartz-eye sericite schist (QESS), the quartz- sericite schist (QSS), the quartz-eye porphyry (QEP) and the weakly sericitic felsic volcanic (QR). The QESS and the QSS units are virtually identical except that the QESS unit contains up to 5% lenticular quartz-eyes, l-3mm in length. The same relationship is visible between the QEP and the QR. The QESS/QSS units contain ID-50% sericite, trace-5% feldspar, trace biotite, trace-3% pyrite, and the rest is quartz. Most of the sericite has been metamorphosed into coarser grains and is probably muscovite. Often sericite is found lining or adjacent to fractures. West of Line 27400E, the QSS and QESS units are dominant. East of Line 27400E and especially 300m past Pickerel Bay, the QEP and QR units begin to become more prevalent."5
The sericitic package is approximately 20m thick. West of Gouda Lake, the package consists of quartz-sericite schist (5m) overlain by a quartz-eye sericite schist (5m) which is capped by quartz-sericite schist (10m). The upper quartz-sericite schist unit (QSS) contains 10 to 403; sericite with minor biotitic bands. The quartz-eye sericite schist (QESS) generally contains only lS-25% sericite with 3% lenticular 2-4mm diameter quartz-eyes. The basal unit is slightly less sericitic than the upper QSS. "In the deposit area, a thin semi-massive sulphide lens, up to 30cm thick, is occasionally observed always at or near the base of the sericitic package. Reports by Adamson for Lac Minerals suggest that the higher gold content is not a function of the amount of pyrite in the sericite schist. However, careful analysis of the assay data suggests that the highest grade Au is almost exclusively restricted to these sulphide- rich lenses. The semi-massive sulphides contain up to 60*: pyrite, with traces of pyrrhotite. Within the package, occasional green mica clots and molybdenite streaks are observed in the deposit area. The sericitic alteration continues to be strong to the west of the deposit area, right up to the D.C. Lake Fault.
Changes occur in the horizon east of Line 26800E. The first noticeable change is the location of the QESS. Instead of being in the middle of the sericitic package, it migrates towards the footwall, where it is observed in the stream leading east of Gouda Lake. As it heads east, the QESS unit appears to be in transition to quartz-eye porphyry, as less and less sericite is present. Within the QSS unit, the sericite content drops over a longer strike
Lemaitre, R. (1994): Geology of the Gouda Lake Area (in house report); p.2, 1.13-26
29
length. However, 400m down strike east of Pickerel Bay, both the QSS and QESS have become the weakly sericitic felsic volcanic and the quartz-eye porphyry respectively. The package is up to 35m thick in this area, but likely this is the result of the package's increased competence. Since it is more competent, it is not flattened as much as those parts of the package which have been sericitically altered. It seems that the alteration responsible for mineralization at the Gouda Lake and Thor Lake peters out east of Pickerel Bay. However, much farther to the east along this horizon may still reveal another alteration centre."6
Footwall to the Gouda Lake Horizon is a 10-15m thick amphibole-bearing wacke to arkosic wacke unit, and in the hangingwall, a thin (O.5-2.Om) skin of banded immature metasediments (Sc/BND).
Thor Lake Horizon
The portion of the Thor Lake Horizon that was mapped is situated at approximately 6000N and extends from Line 25400E to 24400E. The Thor Lake Horizon consists of a package of quartz-sericite schists, which is the faulted-off extension of the Gouda Lake Horizon. The horizon was traced from the D.C. Lake Fault westward, for a distance of l km.
"The stratigraphy of the Thor Lake Area is identical to the Gouda Lake Stratigraphy. The poker chip amphibolite (2e), an excellent marker horizon, is present approximately 225m above the sericite schist in both areas. All units strike east-west and dip to the north between 37" and 550 ." 7
"The altered package consisting of quartz-eye sericite schist (QESS), the quartz-sericite schist (QSS), the quartz- eye porphyry (QEP), and the weakly sericitic felsic volcanic (QR), overlies the banded immature metasediments (Sc/BND). The QESS and the QSS units are virtually identical except that the QESS unit contains up to 53; lenticular quartz-eyes, l-3mm in length. The same relationship is visible between the QEP and the QR. The QESS/QSS units contain ID-50% sericite, trace-5% feldspar, trace biotite, trace-3% pyrite, and the rest is quartz. Most of the sericite has been metamorphosed into coarser grains and is probably muscovite. Often sericite is found lining or adjacent to fractures.
Lemaitre, R. (1994): Geology of the Gouda Lake Area (in house report)j p .3, 1.28 to p. 4, 1.13
Lemaitre, R. (1994): Geology of the Thor Lake Area (in house Report); p .l, 1-8-15
30
These units are strongly foliated and often strongly crenulated. Some areas contain green mica. The QEP/QR units contain as much as 10* feldspar, probably albite (from striations) and are generally massive and never crenulated. In the Thor Lake Area, the QEP/QR units are rare, generally QSS and QESS dominate."8
"The massive sulphides are hosted in a weakly foliated, yellow rusty stained equigranular quartz-feldspar-biotite intrusive or felsic volcanic. Only a very small strike length of this unit was exposed and thus makes it difficult to determine its exact nature. Within this unit over a 4m interval, 3 separate massive sulphide zones were identified. The stratigraphically lowest zone is also the largest zone and is approximately 1.5m wide along the surface. The second is located 30cm north of the first zone and is 25cm wide. Another 30cm north of the second zone is a collection of 3 or 4 thin lcm wide massive sulphide "veins".
Generally, the sulphides comprise at least 851; of the total rock volume, although there are patches where the gangue minerals may account for 703;. Gangue minerals appear to be almost exclusively round quartz-crystals, l-3mm in diameter and may be possible remnants of quartz eyes. Some sericite was observed. Sulphide minerals include sphalerite (4-53;), chalcopyrite (trace-2%, rare), pyrrhotite (65%), and pyrite (30%). Grey pods which may be stibnite-rich were also observed. The sulphides are very coarsely-grained and almost certainly recrystallized. The main zone appears to have a slight cross-cutting relationship with the foliation which may suggest that the sulphides formed as a vein. However, due to the recrystallization and high flattening stresses which these rocks have endured, it is also possible that the sulphides have been slightly remobilized from a classic stratiform sulphide body.
Less than 1.5m from the hangingwall contact of the main sulphide lens is a massive quartz-feldspar-porphyry. The QFP is a minimum of 15m wide and contains lS-20% feldspar phenocrysts (4-6mm diameter), up to 5% quartz-eyes (2-3mm in diameter), and 53; biotite. No sulphides were observed. It is very interesting to note the proximal relation of the QFP to the massive sulphides, which may be very important, especially if the sulphide lenses are in fact veins.
On the south shore of Thor Lake, 45m south of theshowing, a white, massive, quartz-porphyritic unit occurswhich contains 53; biotite, and quartz phenocrysts up to lcm
Lemaitre, R. (1994): Geology of the Thor Lake Area (in house report); p .2, 1.7-22
31
in length. It resembles the QFP unit adjacent to the showing, but is much coarser-grained. Previous mapping called this unit the contact of the Pukaskwa Gneissic Complex with the Hemlo Greenstone Belt. The quartz porphyry unit is approximately 85m wide on surface. It is in contact with a typical, massive granite to the south. The granite appears to be similar to those granites in the vicinity of Gouda Lake. 1* 9
Hosted within the quartz-sericite schist, some 365m west of the Thor Lake Showing, is a vein (2mm wide) of green mica (roscolite). The vein cross-cuts the foliation but is also deformed, consistent with the D2 flattening event.
"About 50m to the east, two sericite schist horizons exist. Between the two is a unit tentatively called an immature metasedimentary rock containing minor garnet and magnetite (Sc/GAR/MAG). It is not clear whether the sericite schist package forks into two parallel horizons or whether these are two distinct felsic lenses. The sericite schists are identical to the descriptions provided above. Towards the west, the Sc/GAR/MAG unit becomes more and more garnet and magnetite-rich. On the extreme western end of the present mapping, large garnet clusters, with individual garnets measuring 4-8mm in diameter were observed, with the clusters following banding. Traces to 33; magnetite also observed. Individual grains look identical to coarse amphibole and may be commonly mistaken for it. The matrix is composed of quartz with only minor traces of feldspar. In addition, the unit begins to look more and more like a felsic volcanic instead of a metasediment. It is possible that the garnet and magnetite may be of hydrothermal origin, or the metamorphic equivalents of previous hydrothermal minerals. Some samples contained up to n.0% medium-grained, white albite crystals which may also be hydrothermal in origin." 10
The showing was sampled, and the results, along with the sample descriptions are included in Table 5 on the following page.
"All four massive sulphide samples were elevated in gold with values ranging from 32 to 134ppb Au. In addition, the silver values vary from 29-55g7t. Zinc values were extremely high, the three massive sulphide samples returned
9 Lemaitre, R. (1994): Geology of the Thor Lake Area (in house report): p .3, 1.4 to p.4, 1.1
10 Lemaitre, R. (1994): Geology of the Thor Lake Area fin-house report;; p.4, 1.17-36
TAB
LE #
B:
LJTH
OG
EOC
HEM
ICA
L R
ESU
LTS
- TH
OR
LA
KE
SHO
WIN
G
Sam
ple
Num
ber
FE06
173
FE06
174
FE06
17S
FE06
176
FE06
177
FE08
178
FE06
179
FE06
180
FE06
181
FE06
1B2
FE06
163
FE06
184
FE06
185
FE06
188
Des
crip
tion
Qua
rtz-S
erld
te S
chist
Feld
spar
Am
phib
olite
Qua
rtz-S
erlcl
te S
chist
Mas
sive
Sulp
hide
s
Mas
sive
Sulp
hide
s
Mas
sive
Sulp
hide
s
Sem
i-Mas
sive
Sulp
hide
s
Host
Roc
k of
Mas
sive
Sulp
hide
s
Qua
rtz-F
elds
par-P
orph
yry
Felsi
c Dy
ke
Qua
rtz-S
erlcl
te S
chist
Qua
rtz-S
erlcl
te S
chist
Qua
rtz-S
erlcl
te S
chist
Qua
rtz-S
erlcl
te S
chist
Sam
ple
Type
grab
grab
grab
grab
grab
grab
grab
grab
grab
grab
grab
grab
grab
grab
Au
(ppb
)•S 48 -5 39 32 80 13
4
22 •S -5 -5 10 •5 •5
Ag
(ppm
)-S -5 •S 29 55 34 40 -S •5 -5 -5 •5 -5 •5
As (ppm
)-2 -2 -2 .2 -2 •2 •2 -2 -2 -2 -2 -2 •2 -2
Be(p
pm)
1300
540
880
-100
•100
•100 280
1100
870
460
550
1300
900
800
Hg
(ppm
)•1 -1 -1 2 4 2 •1 -1 •1 -1 -1 -1 -1 •1
Mo
(ppm
)-5 -5 •5 -5 -5 •5 -5 •5 8 15 5 8 •5 6
8b
(ppm
)-0
.2 0.2 •0.2 S 15 8.8
0.8
0.8
0.3
•0.2
•0.2
•0.2
-0.2
-0.2
W
(ppm
)-4 •4 •4 •4 7 •4 •4 •4 7 •4 5 8 •4 -4
Zn
(ppm
)94 N/
A 77 N/A
N/A
N/A
N/A
150
124
111
77 •50
•50
109
32
33
zinc values of 1.171;, S.16% and 5.143;. The antimony values range from 5-15ppm Sb, and barium was below detection limits. Only a small area of massive sulphides has actually been uncovered.
The sericite schist units around the showing do not show significant Au, Ag, As, Sb, Mo, or Hg concentrations. However, a sample taken from a lens, which is located between the 2c and the quartz-sericite schist, containing 5* pyrite with very coarse biotite returned 46ppb Au, and 2450ppm Zn. This unit may be the result of hydrothermal processes, and suggests the possibility that some or all of the gold may be concentrated in the units adjacent to the sericite schist instead of within the schist itself. 1* 11
4.0 CONCLUSIONS AND RECOMMENDATIONS
The mapped area consists of a northerly dipping package of metasediments and metavolcanic rocks which are sandwiched between the Pukaskwa Gneiss Complex to the south and the Cedar Lake Pluton to the north. The easterly trending Hemlo Fault, which is interpreted as a northerly dipping, layer-sub-parallel, thrust fault, separates the supracrustal rocks into approximately equal east-west trending halves. The northern belt is comprised of clastic metasedimentary and dominantly intermediate metavolcanic rocks, whereas the southern belt consists of clastic metasedimentary and mainly mafic metavolcanic rocks. According to Muir(1982), the north half would be defined as the Heron Bay Sequence and the south half, the Playter Harbour Sequence.
The rocks have been metamorphosed to the sillimanite- almandine-orthoclase subfacies of the almandine-amphibolite facies which suggests temperatures and pressures in excess of 6800C and 6kb respectively.
Two phases of ductile deformation (D2 and D 3 ) have been observed, and there is no evidence of the D l event within the area mapped. In all cases the supracrustal rocks have a well developed S2 foliation while the S, compositional banding is generally restricted to the sedimentary rocks. The S } (crenulation cleavage) is generally most intense proximal to the more competent bodies such as the Cedar Lake Pluton and the Pukaskwa Gneissic Complex.
Within the North Belt, both the S, (compositional banding) and S2 (foliation) dip northward and vary from 320 to 750 and 41"
11 Lemaitre, R. (1994): Geology of the Thor Lake Area fin-house report) ; p.5, 1.22-41
34
to 72", respectively. The dips are generally shallower in the southern portion of the belt and steepen in the northern part. The supracrustal rocks are tightly to isoclinally folded about an easterly trending F2 synformal axis. The axial plane dips northward at 450 to 610 , and the axis plunges westward at 170 to 330 . The plunge is steeper in the western part of the area, and shallows out in the eastern portion. Minor displacements are caused by late, high angle, normal faulting.
Within the South Belt, there is no evidence of a major fold axis, however, the rocks do exhibit a strong, easterly trending, penetrative S2 foliation. For the most part, both the Sj compositional banding and S2 foliation dip northward and vary from 06" to 620 and 050 to 700 , respectively. The dips are shallowest proximal to the contact with the Pukaskwa Gneissic Complex. Late, high angle, normal faulting strikes northeast and northwest, and, except for the D.C. Lake Fault where the offset is in the order of 950 metres, displacements are generally minor.
In the North Belt, the Upper Anomalous Horizon represents the only evidence of felsic volcanism. It consists of rhyolitic ash, lapilli and crystal tuffs which host weak to moderate sericite alteration with 2 to 3!* (locally ID-15%) disseminated pyrite. There is no evidence of hydrothermal alteration adjacent to this unit.
The Rust Lake Quartz Porphyry consists of 5 to 103; flattened quartz eyes in a felsic matrix which is moderately altered with 15 to 251; sericite. Pyrite is very fine grained and occurs as disseminations that range from 2-3* and locally S-10%. Based on rare earth data, compositional, alterational and textural similarities, the Rust Lake Quartz Porphyry comes very close to being a Noose Porphyry "look-alike". Footwall to the Rust Lake Quartz Porphyry is a garnetiferous sedimentary unit which may represent the metamorphic facies equivalent of argillic hydrothermal alteration.
The East Grid Showing consists of a northeasterly dipping, weakly sericitic, intermediate volcanic unit that measures 9 to 13m in thickness. The mineralization is fracture controlled and consists of 3-53; pyrite with trace to 13; molybdenite. One sample returned 32ppb Au while the remainder were below detection limits. The showing is spatially associated with a deformed body of quartz-feldspar porphyry that is proximal and sub-parallel to the main F2 fold axis. Although the lithogeochemical results were disappointing, the important point is the possible relationship with the quartz-feldspar porphyry and its proximity to the main F2 fold axis. This suggests that the fold axis may have been the structure that controlled emplacement of the porphyry and resulting mineralization.
The only evidence of felsic volcanism in the South Belt are the Gouda Lake and Thor Lake Horizons. These are considered to
35
be the same and have been mutually offset by the right lateral D.C. Lake Fault. The horizons consist of four distinct subunits; the quartz-eye sericite schist, the quartz-sericite schist, the quartz-eye porphyry and the weakly sericitic felsic volcanic. The intensity of alteration decreases east of Pickerel Bay and appears to increase in a westward direction from the Thor Lake Showing.
Within the Gouda Lake Horizon, the highest gold grade is restricted to a thin semi-massive sulphide lens at or near the base of the sericitic package.
The Gouda Lake Deposit is open at depth and, according to Lac Minerals, has an inferred resource of 167,000 tonnes at 3.5lg.'t Au, based on 50m polygons. As the drill hole spacing is q .orally greater than 50m, potential resources may exist in the iaces between.
Near the D5 fold on the east shore of Gouda Lake, the mineralized horizon is very flat lying over a fairly large area and has only been tested by one drill hole. The area north and east of this hole is largely untested.
There is evidence of hydrothermal activity along the Thor Lake Horizon, as:
i) a quartz-feldspar porphyry body occurs hangingwall to the massive sulphide showing,
ii) there are local occurrences of garnet and magnetite which may represent metamorphic equivalents of hydrothermal alteration minerals.
As a result of the mapping program, the following recommendations are made:
i) Within the North Belt, the main F2 fold axis may be the structure that controlled emplacement of the felsic porphyry bodies. Exploration should be concentrated along this structure.
ii) The Rust Lake Quartz Porphyry is an attractive Hemlo-type target. Although, in the immediate vicinity, this was drilled to depth, no previous effort was made to evaluate the porphyry along strike. Further exploration efforts should be concentrated along the strike extension.
iii) Along the Thor Lake Horizon, it appears that thealteration intensity -increases in a westward direction. Thus, future exploration programs should be concentrated west of White River and progress towards Frank Lake.
36
5.O BIBLIOGRAPHY
Archer, B., Shevchenko, G. (1994):Geological and Geochemical Surveys conducted on the White River Property "Tail"; Assessment Report submitted by Placer Dome Canada Limited.
Fowler, T.J. (1994):Sheeted and Bulbous Pluton Intrusion Mechanisms of a Small Granitoid from Southeastern Australia: Implications for Dyke-to-Pluton Transformation During Emplacement; Tectonophysics 234
Harris, D.C. (1989):The Mineralogy and Geochemistry of the Hemlo Gold Deposit, Ontario; Geological Survey of Canada Economic Geology Report 38.
Johnson, P., Mason, R., Kusins, R. (1994):The Relationship of the Hemlo Gold Deposit to a Felsic Intrusive Complex (unpublished interim report;
Kuhns, R.J. (1986):The Golden Giant Deposit, Hemlo, Ontario: Geologic and Geochemical Relationships Between Mineralization, Alteration, Metamorphism, Magmatism and Tectonism; unpublished PhD thesis, University of Minnesota, Minneapolis, Minnesota.
Muir, T.L. (1982):Geology of the Hemlo Area; Ontario Geological Survey, Report 217.
Muir, T.L. 1993:The Geology of the Hemlo Gold Deposit Area; Ontario Geological Survey, Open File Report 5877.
Shevchenko, G. (1994):Humus Geochemical Surveys conducted on the White River Property "Main Block"; Assessment Report submitted by Placer Dome Canada Limited.
Winkler, H.G.F. (1967):Petrogenesis of Metamorphic Rocks, 2nd Edition
Winkler, H.G.F. (1976):Petrogenesis of Metamorphic Rocks, 4th Edition
APPENDIX l
STATEMENT OF COST
STATEMENT OF COST
WHITE RIVER PROPERTY - 1994 GEOLOGICAL SURVEY
LABOURS. BeauchampD. GoyetteC. GreenZ. HuntR. LemaitreA. MaceB. NelsonM. SellersG. Shevchenko
51 15 24 21 70 24 62 14 72
mandays mandays mandays mandays mandays mandays mandays mandays mandays
e e e e e e e e e
S 147 /day 5130/day 9135/day SlOO/day Siei/day SlOS/day 5161/day S 113 /day 5261 f day
Sub-Total
7,497. ao 1,950. 00 3,240. 00 2,100. 00
11,270. 00 2,520. 00 9,982. 00 1,582. 00
18.792."
558,933. 00 958,933.'
COMTRACTOR COSTSH.A. Barclay Exploration Services (30 days) Vytyl Exploration Services (133.7km)
Sub-Total
17,514. 00
S0.811. 00
S68,325. 00 968,325.'
LOGISTICSRoom St BoardVehicle ExpenseGPS RentalFreightCommunicationComputer RentalTravelField Supplies
383 mandays 9 S42. 7(Ymanday383 mandays e SlS.
7 units for 2 months
2 months @ 55807mo
Sub-Total
16,469. 10 7,085. 9,100. 00
415. 00 1,550."" 1,160. 00 3,940. U0 8.600. 00
S48,319. so 948,319. :
TOTAL 9175,577.'
APPENDIX li
NATURE OF THE EAST GRID GOSSAN
R. Lemaitre
Geological ReportSeptembers, 1994
by Roger LemaitreSenior Mapping Geologist
White River Project 505E
Nature of the East Grid Gossan
Location
During activities this field season, two old trenches were discovered along the eastern end of the East Grid. The first trench was discovered approximately 50m east of Line 30600E, between 7425N and 7675N . The second trench is located 50m east of Line 30400E, between 7675N and 7875N. Both trenches are oriented roughly in a north-south direction but tend to be snaky with very few straight stretches. Both trenches are also very old, between 10 and 30 years old, based on estimates taken from rings of small trees nearby. This predates Lac Minerals' own exploration program. Likely, the trenches were not discovered by Lac during their work.
Local Geology
In the east grid area, there are 5 main rock types, not including later intrusive units. These rock types are mafic volcanics (unit 2), intermediate volcanics (unit 3), immature metasedimentary rocks or wackes (unit 5), feldspathic metasedimentary rocks (unit 6), and quartzose metasedimentary rocks (unit 7). In the western section of the grid, these units are parallel and appear to be part of nice east-west striking, 450 north-dipping layer-parallel stratigraphic section. However, along the eastern portion of the grid, a large, first-order, second generation tight to isoclinal fold nose is present (see East Grid Map). From the available magnetic maps, it seems that this major closure's axial trace roughly trends WNW, and proceeds through the Yellow Birch Lake Fold and continues through the entire property.
The area of interest lies near the contact of an intermediate volcanic unit and feldspathic metasediments. A
large, deformed body of Quartz-Feldspar Porphyry is located near the fold nose, in the vicinity of the eastern trench.
Trench Geology
The geology of the trenches is plotted on the East Grid Map (Fig.l). In addition, due to it's structural complexity, the eastern trench was mapped at a 1:1000 scale and is included at the back of this report.
There are four main units in the trenches; intermediate volcanics, the gossan, feldspathic metasediments, and quartz- feldspar porphyry. Minor feldspar porphyry, mafic dykes, and quartz veins are also present.
The footwall contact of the gossan is located approximately 5m above the intermediate volcanic/feldspathic metasediment contact. The gossan ranges from 15m wide on surface in the eastern trench to 10m thick in the western trench. Banding dips roughly WNW at 650 , and the foliation is east-west dipping 60-700 north.
The intermediate volcanic unit is composed of two subunits, a massive tuff/flow (3a), and a crystal tuff (3b) . The 3a unit is light-grey-blue in colour and contains approximately S-15% biotite, 153; quartz, and 70-803; feldspar. Biotite has a preferred mineral orientation which defines a weak foliation. The unit is sometimes banded with bands being several centimetres thick. The mineralogical difference between the bands is minute, being defined by only small changes in the biotite concentration. The unit is very competent and does not break easily. Occasionally, l-2mm diameter feldspar crystals are observed. The 3b unit is dark to light-grey in colour and contains patchy feldspar phenocrysts ranging from 2-10mm in diameter. The phenocrysts are anhedral to subhedral with occasional rotational fabrics, pressure shadows, and foliation wrap-around textures.It is estimated to contain 401 quartz, 401 feldspar, lot biotite, and 53; possible sericite.
The gossan zone itself is composed of dark grey, fine to medium-grained interlocking quartz crystals with minor sericite/muscovite and traces of biotite. The unit contains several fractures which host 3-53; (often rusted out) pyrite. Microscopic analysis showed traces of a red mineral which appears to be cinnabar. Also a silvery, soft mineral is present, from trace to 13;, which according to the assay results is likely molybdenite. Staining on one sample from the west trench showed up to 10t fine K-spar was present but usually, K-spar was absent. Also present are some unusual grey pods, 10-50cm in diameter,
which contain up to 103; pyrite, abundant stibnite/molybdenite and are very siliceous. These pods do not seem to contain different metals or differ greatly in their concentrations when compared to the rest of the gossan.
The feldspathic metasedimentary unit (6a) is present on the hangingwall and footwall sides of the intermediate volcanic units. In the trenches, only the footwall side is exposed. The unit is fine to medium-grained, white to tan coloured, containing 53; fine biotite flakes, 603; feldspar, 253; quartz, and trace pyrite. The unit is strongly foliated and only sometimes banded.
The quartz-feldspar porphyry unit is an intrusive body. A large body of QFP is found 60m west of the eastern trench from 7500N to 7550N. Several small dykes of QFP are present in the eastern trench while only one small dyke is present in the southern most section of the western trench. The unit is white to tan coloured, medium to fine-grained containing 5-103; feldspar phenocrysts and 1-23; quartz phenocrysts ranging from O.5-2.5mm in diameter. The matrix is composed of 53; amphibole needles, 153; quartz, with the rest being feldspar. The unit is weakly foliated and in some places, very strongly folded, consistent with the F2 event.
Structural Geology
As mentioned previously, the trenches are located near the nose region of a folded package of intermediate volcanics and feldspathic metasedimentary rocks. This large structure was defined primarily from the data obtained from these trenches.
The dominant style of deformation is tight to isoclinal, moderately dipping, moderately west plunging synform, related to the D2 deformation event. In the area around the trenches, banding and foliation are at sharp angles to one another. Foliation is seen without exception, to penetrate through the noses of minor folds, and is undeformed although some cleavage refraction was noted in some folds. In the east trench, deformation is very strong since it is near the nose region. Deformation in the west trench is far less pronounced, as it is farther from the hinge. However, the axial trace of the fold seen over the entire East Grid is not a straight line as would be expected. Possibly, slight deformation of the F2 axial surface by the D3 event has occurred to cause this warping event, though evidence for such in the rocks is lacking. Since most of the deformation is exhibited in the east trench, interpretation of the deformation will be done primarily from the data obtained from this trench.
Upon examination of the gossan in the eastern trench, it was observed that there was at least one boudinaged diorite dyke present and some fine quartz veins which were folded consistent with the D2 flattening event. Also it was noted that the boudinaged dykes were unaltered and contained no sulphides as observed throughout the rest of the gossan. This piece of evidence, supported by the folded quartz veins suggest that the gossan forming event preceded the dyke intrusion which also preceded the D2 event (it has been shown that the D2 event was responsible for the boudinage of almost every dyke in the area). This combined with the fact that the gossan appears to be conformable with the sediments and volcanics suggest that any mineralization within it will be subjected to the same deformation as the host units and will thus be folded around the nose of the regional structure.
Within the eastern trench, second, third, and fourth order F2 folding is observed. Second order folding is at the scale of 1-2 m, third order folding at the 10-4Ocm scale, and fourth order folding at the centimetre scale. Several order of folding are commonly superimposed upon one another. In the eastern trench, Z-folds are dominant, especially in the central and northern sections. Some second order M, S, and W folds were also observed. It is believed that the W-fold noted on the map is the nose of a second order fold near the nose of the major structure, which lies at or near the area noted to contain S and M folds. Thus it would appear that in the east trench, the gossan zone lies on the north limb of the major structure, near its nose and probably continues around the nose and onto the south limb, where it is presently unexposed.
It is also interesting to note that the QFP unit has been folded by the same event, yet it was also seen to acutely cross cut the weak banding of the metasediments. This suggests that the QFP is intrusive and was emplaced prior to the D2 deformation.
Lithogeochemical Results
In the area around both trenches, fourteen samples were collected and sent for analysis for Au, Ag, Mo, and other metals. Enclosed in the Appendix is a table of the results obtained. At the east trench, three samples were taken, one each from areas near the footwall contact, centre, and hangingwall contact. Samples of the QFP unit in the trench and vicinity were also taken. At the west trench, samples were also taken in the same manner. In addition, a loose grab sample comprised of one of the grey pods mention above was obtained. Samples were also taken of small pyrite-bearing lenses in both the hangingwall and footwall
sides within the 3a unit were also sampled (3a,PY).
Unfortunately, almost none of the samples returned any Au or Ag values above 5ppb. Even the Zn values were low, although they were generally higher in the west trench, averaging over 100 ppb. Indicator elements such as As, Sb, and Hg are at or below detection levels. Two of the gossan samples from the east trench, and the three hangingwall 3a,Py lenses in the west trench contained higher than detection level molybdenum. The higher No in the east trench gossan samples can be easily explained by the previously mentioned presence of molybdenite. However, the cause of the slight Mo in the 3a,Py samples cannot be explained. Of interest is sample FE06218 which ran 32ppb Au, the only such sample to exceed the detection level. It is one of the hangingwall 3a,Py lenses.
Conclusions and Recommendations
Despite the lack of any reasonable assay values taken from the gossan in the East Grid area, this area should not be dropped or ignored completely. The grid mapping has shown a few outcrops in the vicinity of the nose of the fold which are part of a fairly large QFP body, minimum 25m in thickness. Due to the poor exposure in this area, it has been difficult to determine the actual extent and orientation of the QFP. There is a good possibility that it could extend for a fair strike length to the west and even could continue through the nose of the fold to the east. Future work in this area should include:
1. Extend the east trench southward by 50-75m to determine if the gossan actually comes around the nose of the fold. Small amount of trenching along the projected north and south limbs will probably be necessary to expose more of the gossan since its exposure is limited.
2. Prospecting along the QFP unit, both eastward butprimarily westward to determine its limits. Traces of QFP and FP were noted in some of the lines to the west.
Roger LemaitreSenior Mapping Geologist
Sam
ples
Tak
en N
ear t
he T
renc
hes -
Eas
t Grid
- W
hite
Rive
r Pro
perty
Samp
le No
FE06
201
FE06
202
FE06
203
FE06
204
FE06
206
FE06
211
FE06
212
FE06
213
FE06
214
FE06
215
FE06
216
FE06
217.
FE06
218
FE06
219
Unit -
Loca
tion
OoM
Wi-F
WiU
*
Oow
tn •
Cent
ra
Oot
un -H
W li
d*O
FP-W
mw
Ml
OF
P.M
wlP
MO
ouM
'FW
fld*
OoM
wH
Wtid
*O
otun
-looM
StP
y-FW
iU*
Qoi
tifi -
CwN
ra3*
-00*
329
3*,P
y- 0
0*32
93t
,Py-
00*
330
3*,P
y. 0
0*33
0
Tren
chEa
stEa
stEa
stEa
stEa
stW
est
Wes
tW
est
Wes
tW
est
Wes
tW
est
Wes
tW
est
AU •8 6 •6 •5 •6 •5 •6 •6 •5 •5 •6 •6 32 •6
AQ •5 •5 •5 -6 . . . - . . •6 •6 •5 •5
AS •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2 •2
BA 440
•100 34
077
082
024
075
051
060
062
031
034
025
048
0
BR . * . . . . . . . . . . . -
CA3 9 3 3 2 2 2 1 •1 3 4 3 7 3
CO 13 28 6 10 16 90 26 29 16 24 19 61 36 32
CR 86 405 97 46 70 50 34 32 69 60 93 79 440 38
CS 11 4 9 4 6 6 9 6 9 7 e 6 •2 6
FE 2.58
6.66
4.43
2.90
3.96
6.54
8.30
7.40
3.67
7.73
3.75
5.66
6.30
2.66
HF3 2 4 3 6 3 3 3 4 5 4 3 2 3
HO . . * * . . . * * . * * * *
IR •5 •6 •5 •6 •5 •5 •S •5 •5 •5 •5 •5 •5 •S
MO
270 •6 36 •6 •5 •5 •6 5 •5 8 •6 43 12 60
NA34
400
1227
024
200
3320
043
700
3250
016
600
1760
01
3960
029
800
2240
027
200
2080
022
200
Nl
•60
•60
•50
•60
•60
•60
160
160
•60
100
100
240
•60
130
RB 77 •30 66 66 39 32 81 39 63 63 68 61 •30 49
SB •0.2
•0.2 0.3
•0.2
•0.2
•0.2
•0.2
•0.2
•0.2
•0.2
•0.2
•0.2
-0.2
•0.2
SB
lflD
w N
OFE
0620
1FE
0620
2FE
0620
3FE
0620
4FE
0620
5FE
0621
1FE
0621
2FE
0621
3FE
0621
4FE
0621
6FE
0621
6FE
0621
7FE
0621
8FE
0621
9
IMS-
loca
tion
OoM
tn-F
Wtb
*GO
MWI -
Ccn
lrtO
omn-
HW
iB*
OFP
-SO
mwM
lO
FP-n
wS
Prt
Got
ttn.F
Wtld
*O
otun
.HW
ild*
Oot
un -
loot
*3t
.Py-
FWtU
*Q
oiun
-Ctn
M3*
-00*
389
3*,P
y- 0
0*32
93t
.Py
00*3
303*
.Py-
00*
330
Tren
chEa
st•a
stEa
stEa
stEa
stW
est
Wes
tW
est
Wes
tW
est
Wes
tW
est
Wes
tW
est
SG 11.0
34.0
12.0 7.6
11.0 8.8
6.6
4.8
11.0 9.2
12.0
11.0
35.0 8.7
SE •8 •5 •8 •5 •5 •5 •5 •5 •5 •5 •5 •S •5 •6
SN•0
.01
•0.0
2•0
.01
•0.0
1•0
.01
•0.0
1•0
.01
•0.0
1•0
.01
•0.0
1•0
.01
•0.0
1•0
.01
•0.0
1
SR 0.13
•0.0
5•0
.05
0.15
0.20
-005 0.07
•0.0
50.
150.
090.
12•0
.05
0.10
•0.0
5
TA * m ' . . . - . . . m - . -
TH 1.9
4.0
6.6 1.6
6.0
3.5 1.6
1.1 6.6
2.0
4.8
3.8
2.5
2.9
U 1.2
1.9
1.8
•0.5 1.8
0.9
0.8
•0.5
•0.5
•0.5
•0.5 0.8
•0.5 1.2
W •4 •4 -4 •4 •4 •4 •4 •4 •4 •4 •4 •4 •4 •4
ZN 61 156
103
•50
•60 98 68 52 116 99 173
113
116
432
LA 11 24 28 12 16 17 11 9 24 14 20 19 16 14
CE 22 60 60 31 37 34 21 21 50 27 37 44 35 31
NO7 25 16 •5 12 13 e 12 24 14 14 19 18 15
SM 1.3
6.0
2.1 1.5
2.4
2.6
1.7
1.4
4.6
2.4
2.9
3.5
3.6
2.4
EU 0.7
1.6
0.8
0.6
1.1 1.2
0.8
0.7
1.9
1.1 1.2
1.4
1.4
1.2
TB •0.5
•0.6
•0.5
•0.5
•0.5
•0.5
•0.6
•0.6 0.6
0.6
•0.5
•0.6
•0.5 0.6
YB 0.76
1.96
1.02
0.68
0.63
0.73
0.60
0.41 1.23
0.77 1.25
1.04
1.56
0.92
LU 0.10
0.32
0.17
0.11
0.13
0.12
0.10
0.05
0.20
0.12
0.21
0.15
0.25
0.12
Mas
s28
.28
31.4
627
.97
30.6
025
.64
33.0
039
.36
28.4
531
.12
32.7
430
.74
34.0
430
.60
29.8
1
ANva
lues
lnpp
mM
oapt
Auln
ppb.
Ci.F
e.Sr
.Snl
r^
•Ve s
ign de
note
below
detec
tion l
evel
PL
AC
ER
DO
ME
: C
AN
AD
A L
IMIT
ED
-
SA
MP
LE
RE
PO
RT
PROP
ERTY
NAM
E: W
hite
Rive
r
LOCA
TION:
Ea
st G
rid S
howi
ng
NTS:
42C
/12
UTM
E:
5979
50UT
M N
: 53
9032
0
DATE
: Ju
ly 26
,199
4
TOTA
L #
OP P
AGES
: 3
SAMP
LERS
: R.
Lem
altre
Sam
ple
Num
ber
FE06
201
FE06
202
FE06
203
FE06
204
FE06
20S
Loca
tion
4 D
escr
iptio
n
Out
crop
RL-
94-2
91 -
Eas
t Tre
nch
- Qua
rtz-S
erici
te S
chist
, PY.
STB.
CIN
- Gos
san
- FW
Side
Stro
ngly
alter
ed u
nit, o
nly q
uartz
-pyr
ite a
nd m
inor s
erici
tere
main
ing.
Som
e tra
ces
of b
iotite
?. C
onta
ins s
ever
al fra
cture
s th
atco
ntai
n ab
unda
nt (o
ften
rust
ed o
ut) p
yrite
and
ser
icite
. Be
twee
n th
eau
lphidl
zed
fractu
res
is fin
e-gr
ained
qua
rtz a
nd S
K fin
e dis
sem
inate
dpy
rite.
Po
ssibl
e cin
naba
r obs
erve
d un
der t
he m
icros
cope
. De
finite
stibn
ite o
bser
ved
with
the
micr
osco
pe.
Occ
asio
nal c
oars
e 5
mm
diam
eter
pyr
ite c
rysta
ls.
Out
crop
RL-
94-2
91 -
Eas
t Tre
nch
- Qua
rtz-S
erici
te S
chist
, PY
-Go
ssan Iden
tical
to F
E 06
201
exce
pt ta
ken
from
the
cent
re o
f the
goss
anou
s zo
ne.
Out
crop
RL-
94-2
91 -
Eas
t Tre
nch
- Qua
rtz-S
erici
te S
chist
, PY
-Go
ssan
- HW
Side
Iden
tical
to F
E 06
201
exce
pt ta
ken
from
the
HW S
ide o
f the
goss
anou
s zo
ne.
Out
crop
BN-
94-3
57 -
Quar
tz Fe
ldspa
r Por
phyr
yTa
ken
from
a Q
FP u
nit w
hich
con
tains
5K
med
ium to
coa
rse
euhe
dral
quar
tz p
heno
crys
ts, 1
0K fe
ldspa
r phe
nocr
ysts
In a
quar
tz-
feW
spar
-biot
ite m
atrix
. Th
is un
it ha
s be
en fo
lded.
Lo
cate
d 60
m w
est
of th
e ea
stern
tren
ch.
Outcr
op R
L-94
-291
- E
ast T
renc
h - Q
uartz
-Fel
dspa
r Por
phyr
y - 1
6.70
mfro
m S
P#3
Fine
to m
edium
-gra
ined
unit
cont
aining
5-1
OK
feld
spar
phe
nocr
ysts
and
1-2K
qua
rtz p
heno
crys
ts ra
nging
from
0.5
-2.5
mm
In d
iamet
erAp
prox
imat
ely 5
-10K
am
phibo
le ne
edles
, fine
-med
lum-g
ralne
d.
Mos
tof
the
mat
rix Is
felds
par b
ut a
bout
15t
t of t
he u
nit Is
mat
rix q
uartz
.
Sam
ple
Type
grab
grab
grab
grab
grab
Wid
th(m
)Au (ppb
)-5 5 •5 -5 •5
Ag (ppm
)•5 -5 -5 -5 •5
As(p
pm)
-2 -2 -2 -2 -2
Ba(p
pm)
440
•100 340
770
820
Hg(p
pm)
-1 -1 •1 •1 -1
Mo
(ppm
)N\
A -5 36 -S -5
Sb(p
pm)
•0.2
-0.2 0.3
-0.2
-0.2
W(p
pm)
-4 -4 -4 -4 -4
Zn(p
pm)
61 156
103
-50
-50
Sam
ple
Num
ber
FE06
206
FE06
207
FE06
200
FE06
210
FE06
211
FE06
212
Loca
tion
A D
escr
iptio
n
Out
crop
RL-
94-2
98 -
2c, K
F.PY
.AK
Cont
ains
abun
dant
rusty
frac
ture
s cu
tting
thro
ugho
ut th
e ro
ck.
Appr
oxim
atel
y 1-
5S ru
sted
out p
yrite
In th
e m
assiv
e ro
ck w
hich
Is co
mpo
sed
of 9
0tt f
elds
par a
nd 1
0ft w
ierd
blade
d cle
ar a
mph
ibole?
? (h
as th
e ha
bit o
f am
phibo
le).
The
zone
Is h
oste
d by
a 2
c un
it.
Out
crop
RL-
94-2
98 -
9a,P
Y Co
ntain
s or
ange
-sta
ined
crys
tals
of a
mph
ibol
e (3
5ft),
felds
par
(40t
t) an
d qu
artz
(25t
t).
May
hav
e or
igina
lly c
onta
ined
up to
5tt
pyrit
e bu
t this
has
bee
n we
athe
red
out.
Poss
ibly
a m
etas
ed.
Out
crop
RL-
94-3
09 -
Qua
rtz-S
ericl
te(M
usco
vlte)
Sch
ist
Stro
ngly
cren
ulate
d un
it co
ntain
ing s
ever
al q
uartz
-ribb
on a
nd
quar
tz-v
ein
boun
dlnt
. Co
mpo
sed
of 7
0tt c
oars
e m
usco
vite
(met
amor
phos
ed e
quiva
lent a
fter s
erici
te?)
and
30t
t qua
rtz.
Rusty
co
lour
stro
ng a
long
the
mus
covit
e fla
ke b
ound
arie
s. P
ossib
ly up
to M
py
rite
origi
nally
bef
ore
weat
herin
g.
Out
crop
RL-
94-3
13 -
Se, P
Y.AM
P.BN
D M
edium
-gra
ined,
folia
ted,
and
ban
ded
unit.
Cont
ains
25*
amph
ibole,
trac
e ep
idote
, tra
ce p
yrite
, 5*
quar
tz, a
nd 7
0* fe
ldspa
r. Th
ick a
mph
ibole
seam
s pr
esen
t and
are
the
focu
s fo
r alm
ost a
ll of
the
pyrit
e (3
5* o
f the
ban
d).
Thes
e ba
nds
cros
s-cu
t the
folia
tion.
M
ay b
e alt
erat
ion v
elnlet
s??
-SOu
tcrop
RL-
94-3
28 -
Wes
t Tre
nch
- Gos
san
Zone
, P Y,
STB
- FW
Si
de Co
mpo
sed
of fin
e to
med
ium-g
raine
d da
rk g
rey
Inte
rlock
ing q
uartz
gr
ains
with
3-5
* py
rite
rang
ing fr
om fi
ne to
coa
rse-
grain
ed.
Cont
ains
som
e so
n, s
ilver
y sti
bnite
. Co
ntain
s up
to 1
0* K
-spa
r (alt
erat
ion
mine
ral?)
obs
erve
d by
sta
ining
. Pa
tches
of s
tlbnl
te-ri
ch s
iliceo
us
mat
eria
l with
up
to 1
0* p
yrite
Is p
rese
nt a
s 10
-50
cm p
ods
with
in th
e go
ssan
.
Out
crop
RL-
94-3
28 -
Wes
t Tre
nch
- Gos
san
Zone
, PY.
STB
- HW
Side
Id
entic
al to
FE0
6211
exc
ept t
aken
from
the
HW S
ide
Sam
ple
Type
grab
grab
grab
grab
grab
grab
Wid
th
(m)
Au
(ppb
)
8 -5 -5 6 -S -5
Ag
(ppm
)-5 -S -5 •S -5 -S
As (ppm
)•2 -2 •2 -2 -2 •2
Ba(p
pm)
-100 370
510
230
240
750
Hg
(ppm
)-1 •1 -1 -1 •1 -1
Mo
(ppm
)-5 -5 -5 -5 -5 -5
Sb
(ppm
)
0.4
•0.2
•0.2
-0.2
•0.2
-0.2
W
(ppm
)-4 -4 •4 -4 -4 •4
Zn
(ppm
)
92 124
97 122
98 68
Sam
ple
Num
ber
FE06
213
FE06
214
FE06
215
FE06
216
FE06
217
FE06
218
FE06
21B
Loca
tion
A De
scrip
tion
Outcr
op 3
28 -
Wes
t Tre
nch
- Gos
san
Zone
, PY.
STB
- Loo
se c
hunk
s Co
llecte
d fro
m th
e ar
ea a
roun
d FE
0621
2 fro
m th
e loo
se m
ater
ial
cont
aining
abu
ndan
t stib
nite
(rem
nant
s of
on*
of th
ose
pods
disc
usse
d lnF
E062
11).
Outcr
op R
L-94
-328
- W
est T
renc
h - 3
i. PY
- FW
Side
of G
ossa
n Bl
ack
unit c
onta
ining
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n Zo
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ry fi
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it co
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APPENDIX III
GEOLOGY OF THE GOUDA LAKE AREA
R. Lemaitre
Geological ReportSeptembers, 1994
by Roger LemaitreSenior Mapping Geologist
White River Project 505E
Geology of the Gouda Lake Area
Location
The Gouda Lake Area is located on the South Grid east of Line 26000E to 1km east of Pickerel Bay between 4900N and 5650N. To the east, the favourable horizon continues for several more kilometres. To the west, the favourable horizon is cut by the D.C. Lake Fault, and continues through the Thor Lake Area, an offset of roughly 800m. The Gouda Lake Deposit is found within this area, hosted by the sericitic package west of Gouda Lake. The deposit contains 253,000 tonnes of 4.13gXt Au. One of the objectives of this summer's program was to determine if the potential for increasing reserves was possible and to direct future work in that direction.
Local Geology
Generally, all of the units in the Gouda Lake Area strike east-west and dip to the north at between 2O0 and 50".
According to previous mappers, the base of the stratigraphy in the Gouda Lake Area is the Pukaskwa Gneissic Complex. However, in the area immediately south of Gouda Lake west to the D.C. Lake Fault, this unit is actually a granite which is younger than the Hemlo Greenstone Belt. The granite massive and only very weakly foliated in spots. Several granitic-felsic dykes intrude the area between the granite and the Gouda Lake Horizon which seem to be identical to the granite and actually make determining the actual granite contact difficult. Sometimes it is hard to tell if one is looking at a mafic volcanic with abundant dykes or a granite with mafic xenoliths. At least three generation of dykes have been observed. All cross-cut the units within the Hemlo
Greenstone Belt, and the later dykes cross-cut older ones.
In contact with the granite is the lowest stratigraphic unit in the Gouda Lake Area, an amphibolite. This unit can be up to 100m thick, which greatly exceeds its counterpart in the Thor Lake Area. It is composed of 902; amphibole and only 10* feldspar. The unit has been strongly foliated and subsequently crenulated. Often crenulation cleavage is weakly developed.
Overlying the amphibolite is a 10-15m thick metasedimentary unit. West of Line 26800E, this unit is a banded immature metasedimentary rock (5c). East of Line 26800E, the unit resembles more of a feldspathic metasedimentary rock (6c) although this is based on very little information.
Capping this thin metasedimentary layer is the sericite schist package. This package is composed of four distinct subunits, which are, the Quartz-Eye Sericite Schist (QESS), the Quartz-Sericite Schist (QSS), the Quartz-Eye Porphyry (QEP), and the Weakly Sericitic Felsic Volcanic (QR). The QESS and the QSS units are virtually identical except that the QESS unit contains up to 53; lenticular quartz-eyes, l-3mm in length. The same relationship is visible between the QEP and the QR. The QESS/QSS units contain ID-50% sericite, trace-5% feldspar, trace biotite, trace-3% pyrite, and the rest is quartz. Most of the sericite has been metamorphosed into coarser grains and is probably muscovite. Often sericite is found lining or adjacent to fractures. West of Line 274E, the QSS and QESS units are dominate. East of Line 27400E and especially 300m past Pickerel Bay, the QEP and QR units begin to become more prevalent.
A thin skin of banded immature metasediment (5c,BND) always overlies the sericitic package. It is usually O.5-2.Om thick although it is thicker in other areas. The South Grid Nap shows this unit pinching and swelling along the Gouda Lake Horizon. This is actually misleading because the sericitic package, the 5c,BND, and the overlying unit all outcrop on a steep cliff, and thus it makes it difficult to draw such a narrow unit on the map. The presence of a continuous 0.5m thick unit is odd and perhaps is the result of hydrothermal alteration.
Another thin unit overlies the metasedimentary unit which is an amphibolite. The unit ranges from 5-10m thick and is a foliated but unbanded unit composed of 703; amphibole and 303; feldspar. This unit is almost always found over the sericite package, although sometimes it is not as amphibole-rich and actually resembles a 5c unit.
A mixed package of immature and feldspathic metasedimentary
rocks which is roughly 200m thick overlies the amphibolite. This in turn is overlain by a 300m thick series of mafic volcanics. Most of the series is massive to banded mafic flows, but 20-4Om from the bottom of the series, the marker unit, the Poker-Chip Amphibolite is found. It is a distinct unit repeated no where else in the stratigraphy and can be traced across the D.C. Lake Fault to the Thor Lake Area.
Geology of the Gouda Lake Horizon
The Gouda Lake Horizon is defined by the felsic volcanic- sericite schist package and the thin metasedimentary and amphibolitic units immediately adjacent to it. The Gouda Lake Horizon was investigated from the D.C. Lake Fault to approximately 750m east of Pickerel Bay. A program which included surface mapping, prospecting, and logging existing drill core was used to determine the nature of these units.
The Gouda Lake Deposit is situated within the Gouda Lake Horizon between L26200E and L26800E. The deposit contains 253,000 tonnes of 4.13gXt Au and is hosted within the sericitic package. The deposit itself has been intersected by nearly 20 diamond drill holes.
The sericitic package is approximately 20m thick. West of Gouda Lake, the sericitic package is composed in a specific manner. The top 10m of the package is comprised of the Quartz~ Sericite Schist unit (QSS). This unit contains anywhere from ID- 40% sericite, and often contains minor biotitic bands. Below this unit is a 5m segment which is exclusively composed of Quartz-Eye Sericite Schist (QESS). Generally, this unit contains only lS-25% sericite and 3t lenticular 2-4mm diameter quartz- eyes. The lowest 5m of the package is composed of more QSS, which may contain slightly less sericite than the upper QSS. In the deposit area, a thin semi-massive sulphide lens, up to 30cm thick is occasionally observed always at or near the base of the sericitic package. Reports by Adamson for Lac Minerals suggest that the higher gold content is not a function of the amount of pyrite in the sericite schist. However, careful analysis of the assay data suggest that the highest grade Au is almost exclusively restricted to these sulphide-rich lenses. The semi- massive sulphides contain up to 603; pyrite, with traces of pyrrhotite. Within the package, occasional green mica clots and molybdenite streaks are observed in the deposit area. The sericitic alteration continues to be strong to the west of the deposit area, right up to the D.C. Lake Fault.
Changes occur in the horizon east of Line 26800E. The first noticeable change is the location of the QESS. Instead of being
in the middle of the sericitic package, it migrates towards the footwall, where it is observed in the stream leading east of Gouda Lake. As it heads east, the QESS unit appears to be in transition to Quartz-Eye Porphyry, as less and less sericite is present. The within QSS unit, the sericite content drops over a longer strike length. However, 400m down strike east of Pickerel Bay, both the QSS and QESS have become the Weakly Sericitic Felsic Volcanic and the Quartz-Eye Porphyry respectively. The package is up to 35m thick in this area, but likely this is the result the package's increased competence. Since it is more competent, it is not flattened as much as those parts of the package which have been sericitically altered. It seems that the alteration responsible for mineralization at the Gouda Lake and Thor Lake peters out east of Pickerel Bay. However, much farther to the east along this horizon may still reveal another alteration centre.
Structural Geology
Within the Gouda Lake Area, all units generally strike east- west and dip to the north between 2O0 and 500 . Very little evidence for F2 generation folds exist with the exception of some refolded minor F2 folds, few and far between. It is likely that the area sits on the limb of the F2 isoclinal fold found on the East Grid.
However, the deformation noticeably increases to the south. Both the foliation and the banding are folded into open, shallowly east plunging, Z-folds. These folds are related to the later D3 deformational event. In the sericite schist and footwall amphibolitic units, strong crenulation of the foliation is present, which becomes stronger towards the large granite bodies. Near the contact with the granite, crenulation cleavage is developed. However, the granite bodies tend to be massive or at best, only weakly foliated. The crenulation lineation and fold axis of the F, folds plunges approximately l O0 at 0700 . The crenulation cleavage developed strikes east-west and the dip varies from 850 N to 850 S. Since the deformation increases to the south, closer to the granites, it seems likely that the D, folding is the result of a north-south compressional event in which rocks of the belt were squeeze up and deformed over the granites. Most of the D3 folding observed in this area is at less than 2m in scale. Second order folds of 2m wavelength are common, but do not seem to considerably effect the stratigraphy. Third order folds at the 10-3Ocm scale, fourth order folds at centimetre scale, and fifth order folds, at the millimetre- crenulation scale are extremely common and often are superimposed on top of each other. However, only l first order fold was observed in the area. A large, F3 fold is present on the east
shore of Gouda Lake. The attitude of the foliation changes radically and becomes almost north-south striking, and very shallowly east-dipping east of Gouda Lake. The effect of the folding is seen well past Pickerel Bay. Lac Minerals did not identify this folding during their mapping. The sericite schist lies almost flat in this area and has only been tested near shore.
Conclusions and Recommendations
The following are things which may help to increase reserves at the Gouda Lake Deposit:
1. A diamond drill program which plans to intersect the deposit at depth may significantly increase the reserves. The deposit is still open at depth.
2. A drilling program near the D, fold on the east shore of Gouda Lake. The sericite schist is very flat lying over a fairly large area and has only been tested by one drill hole to date. The area north and east of this hole is largely untested and generally unrecognized by previous programs.
3. A near ore reserve calculation should be completed.The existing one is somewhat suspect. It was based on total gold equivalents which is spurious at best and uses polygons with 50m centres. Most of the existing drill holes are over 50m apart at their pierce points and thus a lot of potential reserves may be lost in the spaces in between. Possibly a grade-thickness contour based reserve can yield a more realistic geological reserve in the probable but not proven category. Reserves can be "proven11 by later diamond drilling if necessary.
4. Diamond drilling based on the information which will be gained by the mass balance whole rock program.
Roger LemaitreSenior Mapping Geologist
APPENDIX IV
GEOLOGY OF THE THOR LAKE AREA
R. Lemaitre
Geological ReportSeptembers, 1994
by Roger LemaitreSenior Mapping Geologist
White River Project 505E
Geology of the Thor Lake Area
Location
Thor Lake is located roughly between 25300E and 25400E and from 5950N to 6025N. The Thor Lake Area described herein, is the area 5900N and 6100N from approximately Line 25400E west to White River. The Thor Lake Area contains a package of quartz-sericite schists, which are probably the continuation of the Gouda Lake Horizon on the west side of a large fault structure. This horizon was traced for 1km west of the fault zone.
Local Geology
The stratigraphy of the Thor Lake Area is a carbon copy of the Gouda Lake Stratigraphy. In fact, the Thor Lake Stratigraphy is the continuation of the Gouda Lake Stratigraphy. A north-west striking fault cuts the Gouda stratigraphy near L26000E which reappears at Thor Lake. The "Poker-Chip Amphibolite", (2e) an excellent marker horizon is present approximately 225m above the sericite schist in both areas. All units strike east-west and dip to the north between 370 and 550 .
The lowest unit stratigraphically in the Thor Lake Area is the Pukaskwa Gneissic Complex (PGC). Throughout most of the Hemlo Greenstone Belt, this unit is gneissic. However, in the Thor Lake Area, this unit is not gneissic, and in fact is a granite which is only weakly foliated. In addition, several granitic dykes of similar composition intrude the stratigraphy close to the PGC contact. The lack of foliation and the intrusive relationship of the dykes suggest that the granite in this area is younger than the stratigraphy of the belt.
Above the PGC lies an amphibolite-mafic volcanic unit which contains up to 90t amphibole. It is dark green to black and is
1
of ben strongly crenulated.
Overlying the amphibolite is a 15-2Om thick immature banded metavolcanic, the 5c,BND. This unit contains bands 1-lOcm thick of alternating amphibole-rich (35% amphibole) and amphibole-poor (5%) material. This unit thins out to the west, or is cut off by the PGC granite mentioned above.
The altered package consisting of Quartz-Eye Sericite Schist (QESS), the Quartz-Sericite Schist (QSS), the Quartz-Eye Porphyry (QEP), and the Weakly Sericitic Felsic Volcanic (QR), overlies the 5c,BND. The QESS and the QSS units are virtually identical except that the QESS unit contains up to 5% lenticular quartz- eyes, l-3mm in length. The same relationship is visible between the QEP and the QR. The QESS/QSS units contain lQ-50% sericite, trace-5% feldspar, trace biotite, trace-3% pyrite, and the rest is quartz. Most of the sericite has been metamorphosed into coarser grains and is probably muscovite. Often sericite is found lining or adjacent to fractures. These units are strongly foliated and often strongly crenulated. Some areas contain green mica. The QEP/QR units contain as much as 102; feldspar, probably albite (from striations) and are generally massive and never crenulated. In the Thor Lake Area, the QEP/QR units are rare, generally QSS and QESS dominate.
A thin ^5 m) layer of amphibolite (2c) comprises the hangingwall contact to the sericitic schists. This is unusual because at Gouda Lake, a O.50-1.00m layer of banded metasediments is found between the 2c and sericite schist, and it is absent in the Thor Lake Area. The 2c unit is strongly foliated but not banded and contains a maximum of 752; amphibole.
Overlying the 2c is a 150m interval comprised primarily of feldspathic metasedimentary rocks (6c). Generally they contain 5-103; amphibole. More subunits may be present within this unit since it was not investigated as thoroughly as the lower units during prospecting.The top of the Thor Lake area is capped by a thick sequence of mafic volcanics, the bottom of which is a 5-10m thick amphibolite. This is topped by the Poker-Chip Amphibolite, the marker horizon which is only found near here and roughly in the same stratigraphic position and distance from the sericite schists near Gouda Lake. Above the Poker-Chip unit are the typical massive to banded mafic volcanics.
Geology Around the Sericite Schist - Thor Lake Area
Near the point where the quartz-sericite schist horizon meets Thor Lake, a new massive sulphide exposure was observed.
The outcrop was pristine, never before being struck by a hammer, as it was found beneath a recently blown over tree. Likely, no previous exploration parties found this showing.
The massive sulphides are hosted in a weakly foliated, yellow rusty stained equigranular quartz-feldspar-biotite intrusive or felsic volcanic. Only a very small strike length of this unit was exposed and thus makes it difficult to determine its exact nature. Within this unit over a 4m interval, 3 separate massive sulphide zones were identified. The stratigraphically lowest zone is also the largest zone and is approximately 1.5m wide along the surface. The second is located 30cm north of the first zone and is 25cm wide. Another 30cm north of the second zone is a collection of 3 or 4 thin lcm wide massive sulphide "veins'*.
Generally, the sulphides comprise at least 853; of the total rock volume, although there are patches where the gange minerals may account for 70*. Gange minerals appear to be almost exclusively round quartz-crystals, l-3mm in diameter and may be possible remnants of quartz eyes. Some sericite was observed. Sulphide minerals include sphalerite (4-52;), chalcopyrite (trace- 2\, rare), pyrrhotite (65*), and pyrite (30*). Grey pods which may be stibnite-rich were also observed. The sulphides are very coarsely-grained and almost certainly recrystallized. The main zone appears to have a slight cross-cutting relationship with the foliation which may suggest that the sulphides formed as a vein. However, due to the recrystallization and high flattening stresses which these rocks have endured, it is also possible that the sulphides have been slightly remobilized from classic stratiform sulphide body.
Less than 1.5m from the hangingwall contact of the main sulphide lens is a massive quartz-feldspar-porphyry. The QFP is a minimum of 15m wide and contains 15-20* feldspar phenocrysts (4-6mm diameter), up to 5* quartz-eyes (2-3mm in diameter), and 5* biotite. No sulphides were observed. It is very interesting to note the proximal relation of the QFP to the massive sulphides, which may be very important, especially if the sulphide lenses are in fact veins.
Another intriguing unit lies on the south shore of Thor Lake, only 45m south of the showing. A massive quartz-porphyry unit was found which is white in colour, contains 5* biotite, and quartz phenocrysts up to lcm in length. It resembles the QFP unit adjacent to the showing, but is much coarser-grained. Previous mapping called this unit the contact of the Pukaskwa Gneissic Complex with the Hemlo Greenstone Belt. The quartz porphyry unit is approximately 85m wide on surface. It is in contact with a typical, massive granite to the south. The granite appears to be similar to those granites in the vicinity
of Gouda Lake. Due to time restraints, the strike length of the quartz-porphyry was not determined.
The Thor Lake Horizon between L24400B and L25000E
The Thor Lake Horizon starts to become more and more complex west of Line 25000E. Instead of keeping the exact same stratigraphic order as seen from Line 25000E to the fault and east of the fault along the Gouda Lake Horizon east of Pickerel Bay, slight changes occur.
The first important change is the presence of green mica (roscolite) as a vein in outcrop /632. A thin 2mm wide green mica vein which cross-cuts the foliation was found within the Quartz-Sericite Schist (QSS) unit. The QSS is strongly foliated and crenulated. The green mica veinlet is also foliated and crenulated. The vein is also wavy, a folding style consistent with a vein oriented in the shortening field during the D2 flattening event.
Only 50m to the east, two sericite schist horizons exist. Between the two is a unit tentatively called an immature metasedimentary rock containing minor garnet and magnetite (Se,GAR,NAG). It is not clear whether the sericite schist package forks into two parallel horizons or whether these are two distinct felsic lenses. The sericite schists are identical to the descriptions provided above. Towards the west, the 5c,GAR,MAG unit becomes more and more garnet and magnetite-rich. On the extreme western end of the present mapping, large garnet clusters, with individual garnets measuring 4-8mm in diameter were observed, with the clusters following banding. Traces to 33; magnetite also observed. Individual grains look identical to coarse amphibole and may be commonly mistaken for it. The matrix is composed of quartz with only minor traces of feldspar. In addition, the unit begins to look more and more like a felsic volcanic instead of a metasediment. It is possible that the garnet and magnetite may be of hydrothermal origin, or the metamorphic equivalents of previous hydrothermal minerals. Some samples actually contained up to 101; medium-grained, white albite crystals which may also be hydrothermal in origin.
Structural Geology
The Thor Lake Area is not a structurally complex area. The large D.C. Lake fault, mapped by Lac has been confirmed. The same stratigraphic package south of and including the Poker-Chip Amphibolite through to the Pukaskwa granite is also present at
Gouda Lake. The fault has a dextral offset of approximately 800 m. The stratigraphic units strike east-west and dip at about 4O0 to the north. Only a few isolated minor F2 generation S-folds are present and suggests that this area may be on the south limb of a large isoclinal fold, probably the same one found on the east grid. However, the units near the contact with the large granite bodies exhibit crenulation of the foliation. This crenulation, related to the D3 event, is much weaker than that exhibited by similar units in the Gouda Lake Area. The D3 event is characterized by open Z-folding of the S2 fabric. In fact, the largest F3 generation fold observed spanned only 2m in width. Therefore, the effect of the D3 event on the stratigraphy is minimal and will not significantly effect any predated mineralization.
Lithogeochemical Results - Massive Sulphide Showing
Four samples were taken from the massive sulphide showing (one was a semi-massive sulphide sample), and one sample from the Quartz-Feldspar Porphyry and Host Rock immediately adjacent to the sulphides. The assay results, along with those of other samples from the Thor Lake Area, have been included in the Appendix.
All four massive sulphide samples show elevated gold values, the lowest which was 32ppb Au, the highest 134ppb Au. In addition, significant Ag values were also obtained and were more tightly grouped than the gold, ranging from 29-55 g/t. Zinc values were extremely high, the three massive sulphide zinc values were 1.17 t Zn, 3.16 3; Zn and 5.143; Zn. Antimony values were the highest recorded to date ranging from 5-15ppm Sb. Barium was below detection limits in the massive sulphides. These results are very encouraging. Only a small area of massive sulphides has actually been uncovered.
The sericite schist units around the showing do not show significant Au, Ag, As, Sb, Mo, or Hg concentrations. However, from outcrop #595, a sample taken from a lens between the 2c and the quartz-sericite schist proved to be very interesting. This unit contains 53; pyrite sometimes as stringers and very coarse biotite books (after chlorite??) and is probably the result of hydrothermal processes. It contains 46ppb Au, and 2450ppm Zn. This sample points to the possibility that some or all of the gold may be concentrated in the units adjacent to the sericite schist instead of within the schist itself. Hopefully, this will be observed in the area west of L25000E, where the 5c,GAR,MAG unit is intimately associated with the sericitic units.
Conclusions and Recommendations
The Thor Lake Area has shown excellent potential and is worthy of substantial follow-up work in the near future. Follow- up work should consist of:
1. Drilling of the massive sulphide showing. Somedrilling has been done in the area to the west of the showing, some have indications of semi-massive pyrite and pyrrhotite at the footwall contact with the sericite schist. The elevated Au values, along with the strong Ag and Zn grades obtained warrant a further investigation. Unfortunately, it is unlikely that any more surface exposures of the sulphides can be found. Only 20m to the east is Thor Lake. To the west is a series of swamps and beaver ponds in the direction the sulphides appear to be striking. In addition, a drilling program may help to determine the extent of the Quartz-Feldspar Porphyry unit immediately adjacent to the sulphides. If drilling provides interesting results, the Gouda Lake Area near the fault at L26000E must not be forgotten, since it is the down strike extension to the east and is still needs to be tested by drilling.
2. Continued mapping and sampling of the horizon fromL24400E to the west, across White River to Frank Lake. It appears that this horizon will continue through Frank Lake. A former geologist with Lac confided that a gold showing was found at Frank Lake and was never followed up. In addition, the presence of the 5c,GAR,HAG unit, which increases in thickness, and becomes more garnet and magnetite-rich to the west, coupled with the decreasing distance between the sericite schists and the "fresh" granites and the quartz porphyry indicate this may be a favourable area to investigate.
3. Mapping of the Quartz Porphyry unit on the south shore of Thor Lake. Such a large porphyry body, which has not been previously identified, should be investigated and its extent, and relationship with the sericite schist horizon examined.
Roger LemaitreSenior Mapping Geologist
PL
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along
'qua
sl-str
inger
s'. S
ome
very
coa
rse
3-4
cmch
lorlte
/am
phlbo
le cr
ysta
ls (ch
lorite
afte
r am
phibo
le?) a
re pr
esen
t and
are
poss
ibly
rem
nant
s of
an
alter
ation
eve
nt.
Unit I
s co
arse
-gra
ined.
Outcr
op R
L-94
-598
- Qu
artz-
Seric
lte S
chist
Iden
tical
to FE
0617
3.
Outcr
op R
L-94
-599
- M
assiv
e Su
lphide
s - R
egula
r Sam
pleUn
it co
ntaini
ng a
t lea
st 80
tt su
lphide
s an
d m
axim
um 2
0ft s
ilicate
sav
erag
ing 8
5U s
ulphid
es.
All o
f the
silic
ate g
angu
e mi
nera
ls ap
pear
tobe
qua
rtz.
Cont
ains
up to
10f
t coa
rse
quar
tz cr
ysta
ls wh
ich m
ay b
ere
mnan
ts of
qua
rtz-e
yes?
??.
The
crys
tals
are
1-4 m
m In
diam
eter
and
are
crysta
l clea
r and
free
of I
nclus
ions.
The
sulph
ide c
ompo
sition
(i.e.
80tt
of th
e to
tal s
ulphid
es a
re m
inera
l x) I
s ap
prox
imat
ely 6
5Kpy
rrhoti
te, 3
0tt p
yrite,
2-5
* sp
haler
ite, a
nd u
p to
2tt
chalc
opyri
te.Th
ere
Is als
o th
e po
ssibi
lity o
f oth
er s
ulphid
es s
uch
as s
tibnit
e, bo
rnite
,an
d co
vellit
e, bu
t the
se o
ccur
ance
s ar
e lik
ely ta
rnish
ed p
yrite
and
pyrrh
otite
instea
d of
true
sulp
hides
. Th
e un
it Is
gene
rally
coa
rse
grain
ed a
nd s
ubhe
dral
to e
uhed
ral,
pyrite
cub
es a
re c
ommo
nly 1
cm In
diame
ter.
High
ly me
gnet
lc
Sam
pleTy
pe
grab
grab
grab
grab
Wid
th(m
)Au (PPb
)•5 46 •5 39
Ag (ppm
)-S -5 •5 29
As(p
pm)
•2 -2 -2 .2
Ba (ppm
)13
00
540
880
.100
Hg (ppm
)-1 •1 -1 2
Mo
(ppm
)-5 -5 -5 -5
Sb (ppm
)-0
.2 0.2
-0.2 5
W(p
pm)
-4 -4 •4 •4
Zn (ppm
)94 N/
A 77 N/A
Sam
ple
Num
ber
FE06
177
FE06
178
FE06
179
FE06
180
FE06
181
FE06
182
Loca
tion
ft De
scrip
tion
Outcr
op R
L-94
-5M
- M
assiv
e Su
lphide
s - G
rey
Sulph
ide P
od
A 20
cm
diam
eter
pod
of g
rey
sulph
ide m
ater
ial w
as s
ample
d. Th
eaa
pods
occ
ur sp
orad
ically
thro
ugho
ut th
a zo
na.
Thas
a po
ds a
ra
poss
ibly
galen
a an
d/or
atib
nlte-
rtch.
Tha
sulph
ides
in thi
s zo
ne a
ra
son
and
give
the u
nit a
lead
-gre
y co
lour.
The
zone
app
ears
to be
py
rrhot
lte-ri
ch, I
n ex
ceaa
of 7
5* w
ith 2
5* o
f the
gre
y su
lphide
mi
nera
l.
Outcr
op R
L-94
-599
- M
assiv
e Su
lphide
s - R
egule
r Sam
ple
Identi
cal to
FE0
6178
, exc
ept t
aken
from
ano
ther
loca
tion
on th
a ou
tcrop
. Hi
ghly
mag
netic
Outcr
op R
L-94
-599
- Se
mi-M
assiv
e Su
lphide
s Ta
ken
from
the
mar
gin o
f the
mas
sive
sulph
ides,
It co
ntalna
a m
ix of
the
host
rock
and
tha
mas
sive
sulph
ides.
Conta
lna a
ppro
ximate
ly 30
-50*
pyrr
hotite
, 5*
pyrit
e, 1
0* fe
ldspa
r and
35-
50* q
uartz
. Hi
ghly
magn
etic.
Silic
ate m
inera
ls ar
e lig
ht to
dar
k gr
ey In
colo
ur a
nd a
ra
med
ium to
fine
-gra
ined.
Sulph
ides
rang
e in
size
from
0.5-
20 m
m In
diame
ter.
Outcr
op R
L-94
-599
- 9*
1419
? - H
ost R
ock
of M
assiv
e Su
lphide
s Eq
uigra
nular
, fine
-gra
ined
unit
which
la c
ompo
sed
of a
lmos
t en
tirely
of e
qual
prop
ortio
ns o
f qua
rtz a
nd fe
ldspa
r. Ha
s a
weak
fo
liatio
n de
fined
by ^ m
m th
ick b
ands
whic
h Is
actu
ally
fine
fractu
res/b
ands
con
taini
ng fi
ne d
issem
inate
d py
rite.
Sligh
t ora
nge
staini
ng p
erva
sive
thro
ugho
ut th
e ro
ck.
Outcr
op R
L-94
-599
- QF
P - 9
j Co
ntains
15-
20*
felds
par p
hano
cryata
rang
ing fr
om 4
-6 m
m In
diam
eter
and
up
to S
* sm
aller
2-3
mm
diam
eter
qua
rtz p
heno
crys
t!.
Up to
5*
biotite
, med
ium-g
raine
d, Is
pre
sent
. Un
it is
mass
ive to
we
akly
foliat
ed -
weak
pra
fere
d mi
nera
l orie
ntat
ion h
as b
een
deve
loped
.
Outcr
op R
L-94
-61 3
- 9eW
9g
Mass
ive u
nit w
ith a
pink
colo
uring
with
7-1
0* m
edium
-gra
ined
biotite
, 35*
qua
rtz a
nd 5
5* fe
ldspa
r. Pr
obab
ly th
e do
wn-s
trike
ex
tens
ion o
f FE0
8179
.
Sam
ple
Type
grab
grab
grab
grab
grab
grab
Wid
th
(m)
Au
(ppb
)32 80 13
4
22 -5 -5
Ag
(ppm
)55 34 40 -5 -5 -5
Aa (ppm
)-2 -2 -2 -2 •2 -2
Ba (ppm
)-1
00
-100 260
1100
870
460
Hg
(ppm
)4 2 -1 -1 •1 -1
Mo
(ppm
)-5 -5 -5 -5 8 15
Sb
(ppm
)15 8.
8
0.6
0.8
0.3
-0.2
W
(ppm
)7 -4 -4 •4 7 -4
Zn
(ppm
)N/
A
N/A
N/A 150
124
111
Sam
ple
Num
ber
FE06
183
FE06
184
FE06
18S
FE06
186
Loca
tion
A De
scrip
tion
Outcr
op R
L-94
-618
- Qu
artz-
Sarid
te S
chist
Ty
pical
QS8.
whit
e wt
th ru
sty s
taini
ng a
long
the
relat
ion p
lanes
. So
met
imes
cre
nulat
ed In
the
sligh
tly m
ore
seric
itic s
ectio
ns.
Conta
ins
10-2
5* s
erici
te a
nd tr
ace
pyrite
.
Outcr
op R
L-94
-622
- Qu
artz-
Serid
te S
chist
Id
entic
al to
FE0
6163
.
Outcr
op R
L-94
-625
- Qu
artz-
Serid
te S
chist
W
htte,
cren
ulate
d un
tt wt
th 1
5-25
K se
ricite
end
trac
e py
rtte.
The
rema
ining
75*
Is q
uartz
. Ru
sty a
long
som
e of
the
foVsti
on p
lanes
.
Outcr
op R
L-94
-623
- Qu
artz-
Serid
te S
chist
Co
ntain
s ID
-25%
ser
icite
and
pos
sible
quar
tz-ey
es.
Rusty
alon
g th
e cle
avag
e pto
nces
and
con
telns
up
to 2V
t diss
emina
ted
med
ium-
grain
ed p
yrite.
Fola
ted
to w
eakly
cre
nulat
ed.
Sam
ple
Type
grab
grab
grab
grab
Wid
th
(m)
Au
(ppb
)•5 10 -5 •S
Ag
(ppm
)-5 -5 -5 •5
Aa (ppm
)-2 -2 -2 -2
Ba
(ppm
)
550
1300
000
600
Hg
(ppm
)-1 -1 -1 -l
Mo
(ppm
)5 a -s e
8b
(ppm
)-0
.2
•0.2
-0.2
-0.2
W
(ppm
)5 e -4 -4
Zn (ppm
)77 -5
0
•50
100
APPENDIX V
PROGRESS REPORT ON THE DUCTILE DEFORMATION AT THE WHITE RIVER PROPERTY
W.A. Barclay
W.A. BARCLAY EXPLORATION SERVICES LTD.
23 GRENADIER RD. TORONTO. ONTARIO M6R 1R1. TEL.: 1416) 537-4523. FAX: (4161537-4353
PROGRESS REPORT
on
DUCTILE DEFORMATION STYLE
at the
WHITE RIVER PROPERTY
for
Placer Dome Canada Limited
by
W.A. Barclay
July 15, 1994
TABLE OF CONTENTS
INTRODUCTION l
GENERAL COMMENTS ON DEFORMATION STYLE 2
D2 Deformation 2D3 Deformation 6
MOLSON LAKE TRENCH 7
Orientation Data liImplications 11
GOUDA LAKE AREA 14
Orientation Data 16Implications 17
PRINCIPAL CONCLUSIONS AND RECOMMENDATIONS 18
REFERENCES 20
LIST OF FIGURES
Page
Fig. l Molson Lake Trench, 1:1000 (back pocket) Fig. 2 First, second, and third order asymmetric folds 9 Fig. 3 Expected patterns of folding and boudinage of veins
at different orientations during flattening 13
LIST OF STEREONBTS (appended)
Molson Lake Trench
Contoured Poles to Compositional Banding, SIContoured Poles to Early Penetrative Foliation, S2Contoured Poles to Crenulation Axial Planes, S3Poles to SI, S2, S3, and Misaligned Pegmatite BoudinsMean Orientation of SI and S3, with Contoured Axes of Minor FoldsContoured Axes of Crenulation Lineations, L3Contoured Intersection Lineations, L3Contoured Long Axes of Boudins, L3SI Surfaces and S3 Axial Planes, with L3 Intersection Lineations
North Grid
Contoured Poles to Compositional Banding, SI Contoured Poles to Early Penetrative Foliation, S2 Intersections of Means for Penetrative Foliation fe Compositional
Banding: Molson Lake vs. North Grid Area
South Grid
Contoured Poles to Compositional Banding, SIContoured Poles to Early Penetrative Foliation, S2Contoured Poles to Crenulation Axial Planes, S3Mean Orientation of Compositional Banding and Crenulation Planes,
with Crenulation Lineations, L3 Contoured Axes of Minor Folds
East Grid
Line 284-292E: F2 Fold Axes, and Mean S2 Penetrative Foliation
PHOTOGRAPHIC PLATES
(submitted separately)
INTRODUCTION
The following report describes results of reconnaissance structural
mapping of preserved strain fabrics and deformation style on the White
River property, Hemlo area. Northern Ontario.
Initial field work was focussed on a well-exposed trench located to
the immediate east of Molson Lake, several km west of the current area
of interest. Subsequent mapping along cut lines on the property grid
included the area near and north of Yellow Birch Lake, a region to the
south of White River and west of Pickerel Bay incorporating Gouda Lake
and the contact area of the Pukaskwa Gneissic Complex, and several cut
grid lines south of White River and east of Pickerel Bay. The mapping
in these areas has been intended to obtain a preliminary sense of main
structural patterns, rather than to cover all traverses in detail. It
has been supplemented by on-going field guidance to current members of
the project team in the fundamental concepts and mapping techniques of
applied structural geology.
The field mapping upon which this report is based was undertaken at
the request of Mr. Glenn Shevchenko, Geologist, for Placer Dome Canada
July 15. 1994 White River Project
Limited, South Porcupine, Ontario. This study was carried out between
June 16 and July 15, 1994.
GENERAL COMMENTS ON DEFORMATION STYLE
Strain fabrics attributable to two main phases of regional, ductile
deformation have been recognized thus far in the course of the mapping
of structural elements on the White River property. These are derived
from what are likely the latest ductile events in a tectonometamorphic
sequence which may have been protracted and complex, as has previously
been inferred by Muir (1993), Hugon (1986), and others. It has proved
thus far impossible to read through preserved fabrics in the grid area
to perceive indications of possibly earlier regional tectonic events.
The various structural elements are herein assigned to either D2 or
D3 strain events,- these designations are tentatively correlatable with
D2 and D3 as defined in Muir (1993).
D2 Deformation
The dominant structural grain throughout the property is defined by
the orientation of a cm- to m-scale compositional banding which likely
reflects complexly metamorphosed and transposed stratigraphy. For the
most part, the banding maintains near-uniform attitudes within much of
-2-
July IS, 1994 V/liite River Project
the property area. Its strike is generally to the west with northerly
dips which are typically moderate; slightly steeper dips are discerned
north of Yellow Birch Lake, and somewhat shallower dips occur south of
Gouda Lake near the Pukaskwa Gneissic Complex. Less commonly, banding
rotates more toward WNW-ESE trends, particularly in the latter region.
Similar digressions from the regional east-west trend are noted in the
maps of Muir (1993) around early synkinematic plutons and stocks, such
as the Cedar Lake bodies.
The compositional banding is hereafter in this report designated as
an Si planar fabric. It likely represents, in part, stratigraphy (SO)
which has been regionally transposed. However, it may reflect as well
a superimposed tectonic (metamorphic) segregation banding developed in
individual lithologic units, defined by narrow (generally ^ cm) bands
alternately enriched and depleted in mafic mineral constituents.
All inferred metasedimentary and metavolcanic rocks throughout this
property, and most of the felsic, intermediate, and mafic dykes and/or
sills which are present, exhibit a foliation which is penetrative, and
which is locally continuous to finely spaced. The fabric is typically
defined by the preferred dimensional orientation of inequant amphibole
and biotite grains, particularly evident within quartzofeldspathic and
feldspathic domains. It is locally enhanced by flattened constituents
which pre-date or are synkinematic with respect to the foliation, such
as relatively early porphyroblast and possible porphyroclasts, pheno-
crysts in porphyritic units, feldspar laths in amphibolitic dykes, and
-3-
July 15. 1994 White River Project
various "fragmental" elements (lapilli clasts, etc.). Quartz eyes in
sericite schist and in feldspathic units are similarly flattened where
observed, generally exhibiting dimensional aspect ratios of 2:1 to 3:1
in plan view. The only rocks which do not exhibit this foliation are
relatively late diorite-gabbro, pegmatite, and diabase dykes. In this
report, the foliation (flattening fabric) is hereafter termed S2.
Many outcrop exposures on the property preserve one or more sets of
early dykes, ranging in composition from felsic through to mafic. The
S2 foliation overprints these dykes consistently and, hence, they form
intrusive bodies which are synkinematic with respect to D2. Many have
been rotated toward S2 subsequent to intrusion and commonly show pinch
and swell structure and boudinage. In some cases, inferred extensions
in plan of greater than 1003; are evident along trains of boudins which
were derived from a once continuous dyke. This is particularly true of
some of the more felsic dykes. Less extended boudins linked like thin
sausages along deformed amphibolite dykes have been backrotated toward
the S2 orientation.
In well-banded rocks, this S2 penetrative foliation is consistently
subparallel to compositional banding (SI), within 5-15 degrees of both
strike and dip. This relationship indirectly implies that S2 forms an
axial planar cleavage to straight, long-limbed, isoclinal folds of SI.
Only a few such folds have been discerned thus far. These occur south
of White River from Line 284-288E, roughly from 82+00 to 80+OON. Most
individual exposures there exhibit local, small-scale, parasitic folds
July 15, 1994 Wliite River Project
which are variously Z-, S-, M- and W- shaped. These comprise tight to
isoclinal, long-limbed, overturned, shallowly plunging minor folds, in
which the axial planes are subparallel to the moderately north-dipping
S2 penetrative foliation. Critically, this S2 foliation can be traced
through these fold hinges and describes an axial planar cleavage which
outside of hinge regions lies subparallel to fold limbs. Hence, these
are F2 folds ascribed to D2 regional shortening and flattening defined
by the S2 foliation. The metre-scale folds form series of antiformal-
synlor~Vi pairs in some outcrops, likely congruent to a major regional
s p~irmal closure plunging shallowly WNW.
Most of the few F2 fold axes which have been observed thus far have
shallow to moderate WNW-NW plunge and trend. However, several exhibit
steeply down-dip rakes, particularly where folded continuous bands are
dismembered to form rootless isoclines. Preliminary data in stereonet
describe a distribution along a great circle girdle, which corresponds
with the mean orientation of the axial plane of F2 folds in this area.
Some of the fold axes may have been rotated down-dip after formation.
Thin, short, and generally felsic bands of uncertain protolith have
been noted locally; they are isoclinally folded and transposed to form
rootless isoclines and otherwise dismembered isoclinal fold hinges. S2
is axial planar to these folds.
-5-
July 15. 1994 Write River Project
D3 Deformation
In relatively less competent material, where SI trends more towards
WNW-ESE or NW-SE, and where S1-S2 dips are shallower than normal { ^5
degrees), an additional set of fabrics is well-developed locally. The
set is characterized by asymmetric folds which are long-limbed, gentle
to open, Z-shaped, and shallowly plunging. They form first order fold
structures at m-scale which typically are mimicked by second order cm-
scale rolls, and by third order mm-scale crenulations in lenses, bands
or seams which were relatively less competent than the enclosing rock.
The axial planes of these folds (F3) dip steeply (south, generally) or
subvertically, and locally a weak axial planar crenulation cleavage to
stripey segregation cleavage (S3) is exhibited at this orientation. F3
superimposed folds have generated an associated crenulation lineation,
a strong intersection (S1-S2/S3) lineation, and, uncommonly, a mineral
lineation. The latter is defined mainly by the preferred alignment of
acicular amphiboles, and by the long axes of dyke and vein boudins.
These F3 folds reorient through hinge regions both SI compositional
banding and the S2 penetrative foliation. As well, extended trains of
early dyke boudins can be traced through the F3 fold hinges. Dyke and
vein boudins locally have been realigned toward the S3 orientation and
their long axes often lie along cm-scale F3 fold hinges. Indeed, many
of the smaller-scale F3 folds have been initiated around boudins or at
necks in pinch and swell structure developed along competent layers.
July 15. 1994 White River Project
MOLSON LAKE TRENCH
Many of the strain fabric relationships described above are defined
with unusual clarity along a continuously stripped, 410 m long section
of outcrop on the east side of Molson Lake (the lake is used as a pond
for tailings from the Williams Mine). This stripped section trends at
165 degrees, obliquely across lithologic grain in the area.
The trend from north to south along this trenched outcrop defines a
strain gradient for D3 folding and crenulation. Increasingly pervasive
and intense expression of this superimposed event is discerned towards
the south. In areas which have been less affected by this deformation
imprint, D3-related planar and linear fabrics are restricted in extent
to relatively less competent lithologic components: i.e., those layers
and dykes which were selectively altered prior to the imposition of D3
strain.
For about the first 100 m from the north end of this trench to the
SSE, the dominant tectonic grain is defined by generally thin banding
or compositional layering which is straight, at a mean strike and dip
of about 300/43 NNE. The penetrative foliation S2 is observed in the
leucocratic and more mafic (amphibole- and/or biotite-bearing) layers
(Pla. iii, iv), as well as in felsic to mafic dykes (Pla. ii) cutting
SI banding at a low angle.
This layering uncommonly exhibits minor, open to gentle, shallowly
-7-
July 15. 1994 Wliite River Project
east-plunging, upright Z-shaped folds, the influence of which extends
for less than one to two metres along fold axial traces into adjacent
layers before dissipating. Intersection and mineral lineations, and
crenulation fold axes are observed only within these rare minor folds
and, preferentially therein, within altered relatively less competent
mafic seams and bands. Feldspar-rich bands and layers seldom show an
expression of the D3 folding and associated crenulation fabrics.
The minor asymmetric folds recur with slightly increasing frequency
moving SSE along the trench, but remain restricted in areal extent and
influence for a further 150 m. The D3 crenulation overprint, however,
becomes selectively expressed with an increasing intensity in specific
amphibolitic seams and lenses (Pla. viii, ix, x), many of which likely
are altered remnants of once continuous mafic dykes. The crenulations
are restricted to these mafic seams and immediate contact areas over a
distance of a few millimetres to centimetres.
From about 280 m along the stripped setting and further to the SSE,
the dominant structural style is one of pervasive, first order, metre-
scale, open to gentle Z-shaped folds, the axial traces of which extend
across most of the width of the trench. These are mimicked in geometry
by second-order, cm-scale, asymmetric, Z-folds and, in turn, by third-
order millimetre-scale crenulations (Fig. 2). Strong crenulation fold
axes and intersection lineations (S3/S2 and S3/S1) accompany the folds
(Pla. Il-i) . All first, secondhand third order folds plunge to the E
shallowly, as do intersection lineations. Folds at each scale deflect
fly ae4.efa~Xj
Fig. 2 First, second, and third order symmetric folds
July 15, 1994 White River Project
SI and S2 fabrics through hinges, as well as locally boudinaged felsic
(feldspar porphyry included) to mafic dykes, and altered amphibolitic
seams. Since trains of boudins continue through fold hinges, boudinage
occurred prior to the D3 superimposed shortening. Axial planes of the
folds are subvertical to steeply south-dipping, at an angle of roughly
45 degrees to the dip of SI and S2.
the south end of the stripped trench, two 310 degree trending,
locally weakly porphyritic, felsic dykes mimic the Z- shaped pattern of
folding. They are asymmetrically folded more or less conformably with
compositional banding (Pla. II-iv,v) forming a series of open to close
upright, and locally angular, east-plunging Z-folds. Second and third
order parasitic analogues are strongly developed between the two dykes
and the S3 crenulation cleavage here evolves into an incipient stripey
banding (tectonic segregation cleavage) across layered units (Pla. II-
x) .
Although these two dykes seem at an initial glance to be isotropic.
close inspection reveals that they are foliated, particularly at their
contacts with contiguous layered metasediment s . One comagmatic dykelet
emanates from the larger of the two main dykes here (Pla. Il-vi) . It
is boudinaged through the hinge area and along the limbs of a Z- shaped
fold, from which it is inferred that the source dyke and its offspring
dykelet predated D3 deformation.
-10-
July 15. 1994 White River Project
Orientation Data
Equal-area stereographic plots of poles to SI compositional banding
and S2 foliation reveal weak distributions along great circle girdles.
These girdles are near parallel, and the poles to them lie at 102 - -->
19 and 093 - --> 2 5 respectively. The stereonet patterns confirm field
observations that Si and S2 have been folded about east-plunging axes.
The poles to these girdles are coincident with the mean orientation of
several L3 linear fabric elements, including: axes of minor, Z-shaped
D3 folds (090 - --> 23), crenulation lineations (090 - --> 29), S3/S1 or
S3/S2 intersection lineations (094 - --> 23), and a preferred alignment
of the long axes of dyke boudins (090 - --> 23). The mean orientation
of S3 axial planes and, where revealed, the S3 crenulation cleavage is
090/84 S.
Implications
At Molson Lake, axial surfaces of Z-folds and the parallel, locally
developed, crenulation cleavage approximate the flattening or XY plane
for regionally superimposed D3 shortening. The consistent subvertical
attitude and east-west strike of these fabric elements infer that both
the instantaneous and finite principal strain axes were coaxial with a
shortening direction along a subhorizontal north-south axis. D3 hence
resulted from essentially bulk "coaxial strain (pure shear) rather than
from non-coaxial strain (simple shear). Although Z-shaped folds have
-n-
Jufy 15. 1994 White K\vr Project
been cited as evidence for dextral transcurrent shear elsewhere in the
Hemlo camp (eg. Hugon; 1986) , there is no evidence for the Molson Lake
area or on the White River property that D3 was so constrained.
For coaxial strain, material planes will buckle and/or extend (fold
and/or boudinage) in styles which depend on their initial orientations
with respect to sectors of instantaneous shortening, and instantaneous
extension (Fig. 3). Either Z-shaped folds or S-shaped folds can result
from such shortening, the axial planes of which will lie perpendicular
to the shortening direction. If initially buckled markers rotate into
the extensional field, they will undergo subsequent boudinage (eg. # 3
in Fig. 3). Moreover, the plunges of fold axes generated in initially
buckled material layers by coaxial shortening will depend on the early
attitude of a given layer as well. For example, if line # 5 in Figure
2 represented a high-angle crosscutting pegamtitic dykelet, or quartz
vein, with an east dip, its fold axes after buckling would plunge in a
roughly easterly direction. An initial WNW dip in the same marker can
only generate westerly fold axes.
For non-coaxial strain, on the other hand, fold axial planes within
a discrete shear or deformation zone will exhibit progressive rotation
from the instantaneous flattening plane toward the direction of finite
flattening. Shear-generated fold axes will be deflected progressively
toward the stretch or extension direction moving up a strain gradient.
No evidence of progressive rotation of D3 folds is recorded in the map
area.
-12-
A. B.for. d*formolion
kMi troj*cKKT
B. Aft*r
Fig. 3Helmstaedt .
July 15, 1994 Wliite River Project
GOUDA LAKE AREA
Mapping of structural fabric elements in the south grid area, which
lies south of White River and west of Pickerel Bay, was carried out on
Line 258+OOE north of the tie line, on TL 63+OON from about 274+OOE to
258+OOE, and along an old line (81+OOE) cut for the previous Lac grid,
south of current 63+OON to 49+40N.
Most of the exposures north of Gouda Lake are characterized by thin
compositional banding which is straight and undeflected, and/or by the
early penetrative foliation in all but late pegmatite bodies. Both SI
and S2 exhibit consistent west strikes, and dips which are moderate to
the north. Dips of both conformably become progressively shallower to
the south of Gouda Lake, toward the contact with the Pukaskwa Gneissic
Complex, and foliation within the complex remains shallowly dipping to
subhorizontal at the south end of old line 81+OOE.
A narrow zone in which minor folds are preserved occurs at 57BON on
old L. 81+OOE, along a knoll of mafic gneisses probably derived from a
metavolcanic protolith. These folds are open to gentle, Z-shaped, and
upright, and the area includes a 4-5 m width of cm-scale, second order
parasitic folds which are S-, W-, and Z-shaped through a hinge region.
The axes of the folds are subhorizontal, with an evident slight plunge
to the east of less than 10 degrees. Within the zone of second order
folding, a weak axial planar cleavage is developed, striking west with
steeply north to sub-vertical dip. These folds fold SI and S2, and in
-14-
Jufy 15. 1994 Wnre River Project
style are identical to the asymmetric folds along the trench at Molson
Lake. They are hence inferred to result from D3 strain.
D3 fabrics were not discerned again, moving south on L81+OOE, until
the area of Gouda Lake. The west end of Gouda Lake exposes a thin unit
of quartz-feldspar schist which is locally heavily sericitized with an
overprint of hematite. It locally contains abundant quartz eyes which
have been flattened in the plane of the penetrative S2 foliation.
The upper contact of the sericitic schist with an amphibole-bearing
banded gneissic unit is clean, sharp, and straight. Both units exhibit
strongly developed S2 with equal intensity,- there is no evidence of a
D2 strain gradient moving from one to the other. However, whereas the
overlying laminated gneiss lacks a D3 imprint, the sericitic schist is
intensely crenulated throughout. Crenulation lineations plunge east at
shallow angles or are subhorizontal. A spaced S3 crenulation cleavage
with stripey morphology dips steeply to the north at about 82 degrees.
The S3 fabric strongly crenulates Si and S2.
The sericitic schist contains abundant quartz vein boudins and many
thin aggregates of coarse-grained recrystallized granular quartz. The
boudins are entrained parallel to S2, but more continuous veinlets can
be observed cutting across SI and S2 at a low angle. Several have been
isoclinally folded and now form rootless isoclines. Where these veins
taper at their terminations, narrow 1-2 grain wide ribbons or seams of
quartz extend discontinuously along S2 surfaces, and progressively are
-15-
July 15, 1994 White River Project
disaggregated into single, isolated, flattened, rounded quartz grains,-
these are indistinguishable from the abundant quartz eyes seen in this
unit. Individual grains and many of the vein boudins have locally been
rotated from S2 into the S3 cleavage attitude, and track the shallowly
plunging L3 crenulation lineation.
These fabric relationships suggest that vein quartz emplacement was
pre- to syn-kinematic with respect to D2 deformation. The heavy focus
of D3 crenulation fabrics within the sericite schist probably occurred
because of its relative incompetence resulting from sericitization. D3
postdates the sericitic alteration, which might possibly be related to
the quartz vein introduction.
D3 fabrics persist to the south. Amphibolite along the south shore
of Gouda Lake exhibits cm-scale gentle warps which plunge shallowly to
the east. These appear on dip-slip outcrop surfaces which drop toward
the plunge direction to be more dramatic than they really are, showing
drawn out wisps of feldspar and minor epidote along fold limbs. There
is also a weakly developed stripey segregation cleavage which is axial
planar to these D3 folds.
Orientation Data
Stereonet data for the south grid area show tight clusters of poles
to both SI banding and S2 penetrative foliation at 180 - --> 4 9. These
-16-
July 15, 1994 White River Project
correspond to a mean surface attitude of 270/41 N. Both datasets show
a very weak distribution along great circles, the poles to which occur
due east at a horizontal plunge. The mean attitude of S3 axial planes
and crenulation cleavage is 267/84 N. L3 crenulation lineations occur
at a mean trend and plunge of 083 - --> 11, corresponding to the inter
sections of SI with S3. The few minor folds measured trend NE-ENE, at
shallow plunges.
Implications
The westerly strike extension of sericitic schist along Gouda Lake
is reportedly well-mineralized, and currently is a priority target of
the current phase of exploration on the property.
Fabrics observed within this schist suggest that a mineralized zone
(or mineralization hosted within a competent lozenge-shaped body) will
likely reflect in its finite geometry the preserved D2 and D3 fabrics.
If mineralization predates or is syn-D2, it should lie within, or sub-
parallel to, the plane of S2 foliation, and may conform to some extent
with the trend and plunge of L2 fold axes where developed. In regions
where D2 fabrics have been crenulated during D3 strongly, however, its
initial orientation may be modified by deflection toward L3.
-17-
July 15. 1994 White River Project
PRINCIPAL CONCLUSIONS AND RECOMMENDATIONS
Strain fabrics which are preserved in the region of the White River
property reflect two main ductile deformation events, which may be the
latest episodes in a protracted regional tectonometamorphic history.
Inferred D2 deformation involved intense flattening and development
of long-limbed tight to isoclinal folds. Few are discerned within the
grid area, but those which have been uncovered are likely parasitic to
a major synformal fold closure lying east of Line 288+OOE at about 80+
DON. Observed F2 folds are overturned to the north, and characterized
by axial planes which lie parallel to an S2 penetrative foliation that
is present in almost all lithologies. S2 forms an axial planar fabric
to these folds, cutting folded layers in hinge regions at a high angle
but trending subparallel to F2 fold limbs elsewhere. The limited data
thus far obtained from these folds suggest that they may have variable
plunges in the S2 plane of flattening.
D2 deformation fabrics and transposed compositional banding SI have
been locally overprinted by a D3 crenulation episode. Imprint of this
D3 strain has favoured bands and lithologies which are relatively less
competent than contiguous units, and/or which have attitudes which are
suitable for buckling by N-S shortening along a subhorizontal axis. A
local consequence of D3 strain is that preexisting D2 fabrics may have
been locally reoriented towards S3 and towards the shallow east plunge
alignment of L3 lineations.
July 15. 1994 White River Project
Routine property mapping should incorporate systematic gathering of
structural fabric orientation data. These should be included on plans
of geology, and compiled for stereonet presentation and analysis. It
is of critical importance that F2 folds are distinguished from F3 fold
and crenulation fabrics. Compositional banding-cleavage relationships
for the F2 folds will assist in eventual property-scale extrapolations
of fold patterns.
Respectfully submitted
W.A. Barclay, M.Se.. FGAC Exploration Geological Consultant July 15, 1994; (up-dated April 17, 1995)
-19-
July 15. 1994 Wliite River Project
REFERENCES
Hugon, H., 1986. The Hemlo Gold Deposit, Ontario, Canada: a Central Portion of a Large Scale, Wide Zone of Heterogeneous Ductile Shear,- p. 379-387 m Proceedings of Gold '86 Symposium, an International Symposium on the Geology of Gold, Toronto, Ontario, 1986.
Muir, T.L., 1993. The Geology of the Hemlo Gold Deposit Area. Ontario Geological Survey, Open File Report 5877, 264pp.
-20-
Molson Lake TrenchContoured Poles to Compositional Banding, SI
N = 36k ^ 100.00(Peak - E)7Sigma = 36.4Peak position : 212.0 0/ 46.5'
E = 0.36 Sigma = 0.42
Molson Lake TrenchContoured Poles to Early Penetrative Foliation, S2
N= 22k = 100.00(Peak - EySigma = 19.9Peak position : 215.5 0/ 50.5
E = 0.22 Sigma = 0.33
Molson Lake TrenchContoured Poles to Crenulation Axial Planes, S3
N = 19k = 100.00(Peak - E)7Sigma = 37.4Peak position : O.O 0 / 6.2'
E= 0.19 Sigma = 0.31
Molson Lake Trench: Poles to SI a, S2 o, S3 A , and Misaligned Boudins *.
Molson Lake Trench: Mean Orientations of SI and S3 with Contoured Axes of Minor Folds, L3
N = 24k = 100.00(Peak - E)7Sigma = 44.0Peak position : 90.0 0/ 28.6'
E = 0.24 Sigma = 0.34
Molson Lake TrenchContoured Axes of Crenulation Lineations, L3
N = 33k = 100.00(Peak - E)7Sigma = 49. lPeak position : 90.0 0/ 28.6'
E = 0.33 Sigma = 0.40
Molson Lake TrenchContoured Intersection Lineations, L3
N = 13k = 100.00(Peak - EVSigma = 24.5Peak position : 94.l 0/ 23.1
E = 0.13 Sigma = 0.25
Molson Lake TrenchContoured Long Axes of Boudins, L3
N = 6k = 100.00(Peak - E)7Sigma = 20.3Peak position : 90.00/ 23.3
E = 0.06 Sigma = 0.17
Molson Lake Trench: SI Surfaces and S3 Axial Planes, with L3 Intersection Lineations m .
North GridContoured Poles to Compositional Banding, SI
N= 26k = 100.00(Peak - EVSigma = 10.5Peak position : 202.6 0 / 28.6'
E = 0.26 Sigma = 0.36
North Grid
Contoured Poles to Early Penetrative Foliation, S2
N = 30k = 100.00(Peak - E)7Sigma = 16.3Peak position : 188.l 0/ 22.5'
E = 0.30 Sigma = 0.38
Intersections of Means for Penetrative Foliation Se
Compositional Banding: Molson Lake vs. North Grid
South GridContoured Poles to Compositional Banding, SI
N = 47k = 100.00(Peak - E)7Sigma = 37.5Peak position : 180.00/ 48.6'
E = 0.47 Sigma = 0.48
South GridContoured Poles to Early Penetrative Foliation, S2
N = 40k = 100.00(Peak - E)7Sigma = 28.6Peak position : 180.0 0/ 48.6'
E = 0.40 Sigma = 0.44
South GridContoured Poles to Crenulation Axial Planes, S3
N= 7k = 100.00(Peak - E)7Sigma = 16.6Peak position : 176.6 0 / 6.0'
E = 0.07 Sigma = 0.19
South Grid: Mean Orientation of Comp'l Banding & Crenulation Planes, with Crenulation Lineations L3
N= 11 k = 100.00(Peak-E)7Signu^21.2 Peak position : 82.9 0/ 11.4'
E= 0.11 Sigma = 0.23
South GridContoured Axes of Minor Folds
N= 5k ^ 100.00(Peak - EySigma = 12.8Peak position : 75.l 0/ 14.8'
E = 0.05 Sigma = 0.16
East Grid, Lines 284-292EF2 Fold Axes, and Mean S2 Penetrative Foliation
N = 16k = 100.00(Peak - E)7Sigma = 11.5Peak position : 315.0 0/ 30.0'
E = 0.16 Sigma = 0.28
D DDn DD D Q D D DD n
DLrnn
PLATE ii - Penetrative Foliation (S2) in felsic to mafic dykes
PLATE iii - Penetrative foliation (SJ observed in both leucocratic and more mafic layers
cr
t
C C
i]
D
C CoD Cr O
PLATE iv - Penetrative foliation (S2) observed in both leucocratic and more mafic layers
PLATE viii - D3 crenulation overprint
GC
D DLC
L
r•*
CL
Cr
PLATE ix - D, crenulation overprint
PLATE x - D, crenulation overprint
c
c cr rCL
r
r
L
rn
Ccrr
*
c
PLATE U-i - Strong crenulation fold axes and intersection lineations and
PLATE ll-iv- Felsic dyke asymmetrically folded more or less conformably with compositional banding, forming a series of open to close, upright, and locally angular, east-plunging Z-folds.
cL
cL
rr
DO
Oco
PLATE ll-v- Felsic dyke asymmetrically folded more or less conformably with compositional banding, forming a sehes of open to close, upright, and locally angular, east-plunging Z-folds.
PLATE ll-vi- A comagmatic felsic dyklet emanates from the larger dyke
L
cD
C PLATE ll-x- S3 crenulation cleavage evolves into an incipient stripey banding across layered units.
G CL
Cr
APPENDIX VI
LAB ANALYSIS SHEETS
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REPORT 6769B - MAJOR ELEMENTS FUSION - ICP
CERTIFIED BY :
LERIC L. HOFFMAN
1336 SANDHILL DRIVE ANCASTER. ONTARIO. CANADA L964V5 * TEL 9OS648-9611 * FAX: 905-648-9613
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ACTLABS ACTIVATION LABORATORIES LTD
Invoice No.: Work Order: Invoice Date: Date Submitted: Your Reference: Account Number:
6911 6937
19-SEP-94 31-AUG-94
505E 103
PLACER-DOME CANADA LIMITED BOX 670SOUTH PROCUPINE, ONTARIO PON 1HO
ATTN: GLENN SHEVCHENKO
CERTIFICATE OF ANALYSIS
INAA package, elements and detection limits:
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CERTIFIED BY
DR. ERIC L. HOFFMAN L/ CJ
1336 SANOHIU. DRIVE ANCASTER. ONTARD. CANADA L9G 4V5 * TEL 9O&648-9611 - FAX 9O5-64B-9613
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ACTLABS ACTIVATION LABORATORIES LTD
Invoice No.: Work Order: Invoice Date: Date Submitted: Your Reference: Account Number:
PLACER-DOME CANADA LTD. BOX 670SOUTH PORCUPINE, ONTARIO PON 1HO
ATTN: GLENN SHEVCHENKO
CERTIFICATE OF ANALYSIS
INAA package, elements and detection limits:
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505 104
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CERTIFIED BY :
DR. BJIIC L. HOFFMAN
1336 SANOHLL ORIV/E ANCASTER. CNTARD. CANADA L9G4V5 * TEL 905648-9611 * FAX90&648-9613
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APPENDIX VII
STATEMENT OF QUALIFICATIONS
STATEMENT OF QUALIFICATIONS
I, Glenn Shevchenko, residing at 2869 Dalton Road, Timmins, Ontario, do hereby certify that:
1. I am a graduate of Concordia University (1982) where I received a B.Se. Specializing in Geology.
I have practised my profession part-time since 1977, and full-time since 1984.
3. I am currently employed by Placer Dome Canada Limited and was responsible for the 1994 field exploration conducted on the White River Property.
Date/f m?
Glenn Shevchenko
1.5 SimilARX or mm* r AB
cr -c /* /Tb C* if^ 020 L* 160 O O
Vytyl Exploration Services (2035 Montrose Place, Thunder Bay,Ontario, P7J 1A4) was contracted for the linecutting. There was a total of 28.7km of cut/surveyed line and 146km cut line that was established. The baseline trends east/west with cross lines in a north/south orientation. The line spacing is 200m with a station interval of 25m. The stations are identified with pickets, and metal tags with the inscribed grid coordinate were stapled to them. Although there was a total of 174.7km of line that was established, only 133.7km of the grid was covered by the geological survey.
The geological mapping portion of the 1994 exploration programme extended from June 16th to August 28th (inclusive). Napping was conducted at a scale of 1:2,500 along and between the grid lines. Features were located using hip chain and compass as well as GPS (Global Positioning System).
The geological mapping was performed by S. Beauchamp, R. Lemaitre, B. Nelson and G. Shevchenko, with assistance provided by D. Goyette, C. Green, Z. Hunt, A. Mace and H. Sellers. The digitizing and Autocad drafting for this report was carried out by C. Green and C. Davis. The mapping program was supervised by G. Shevchenko (c/o PlacerDome Canada Limited, Box 960, Timmins, Ontario, P4N 7H1).
W.A. Barclay Exploration Services Ltd. (23 Grenadier Rd., Toronto, Ontario, M6R 1R1) was contracted between June 16th and July 15th (inclusive) to conduct structural mapping and interpretation.
The following table lists the claims and amount of cut line which were actually covered by the geological survey.
Table fi: List of Claims Worked
Claim Number Cut Line (metres)
Claim Number Cut Line (metres)
SSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSM
542588542589542590542591607744607745607746607747607748607749607765607766607767607768607769607770607771607772607787607788607789607790607865607866607867607868607869607870607871607872607873607874607878607879607880
6501100900650350550650800800800600
120012001200800800800400400750700400nilnil375800800800700900900450300
15001300
SSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSM
607881607882607883607884607943607946607947607948607960607961607962607963607964607965607966607967607968607969607970607972607973625556625557625585625586625587625588625589625591625592625593625594625595625597625598
1650nilnilnilnil675600nil7501200120080015007007509001000875450800600nilnil10001150300400800800800800800400600800
Table *l (cent*d)
Claim number
SSM 625599SSM 625600SSM 625602SSM 625603SSM 625604SSH 625605SSM 625606SSM 625607SSM 625608SSM 625609SSM 625616SSM 625617SSM 625618SSM 625619SSM 625621SSM 625622SSM 625623SSM 625629SSM 625630SSM 625631SSM 625632SSM 625633SSM 625652SSM 625653SSM 625658SSM 625659SSM 625660SSM 625661SSM 625664SSM 625665SSM 625666SSM 625667SSM 625668SSM 625669SSM 625670SSM 625671SSM 625672SSM 625673SSM 625674SSM 625675SSM 625676SSM 625677SSM 625678SSM 625679SSM 625680SSM 625681SSM 625682SSM 625683SSM 625684
Cut Line (metres)
700675400800 1000 1200800 1000 1150 1100800450700225200200800 1100250600800nil 1325600 1125 1200 1050450nil1050
75950700700600350400250325600250550800 1100 1200 1200 1200550800
Claim Number
SSM 625685SSM 625686SSM 625687SSM 625688SSM 625689SSM 625690SSM 625691SSM 625692SSM 625693SSM 625694SSM 625695SSM 625696SSM 625697SSM 625698SSM 625699SSM 625700SSM 625701SSM 625702SSM 625704SSM 625705SSM 625706SSM 625707SSM 625708SSM 625709SSM 625710SSM 625711SSM 625712SSM 625713SSM 625714SSM 625715SSM 625716SSM 625717SSM 625718SSM 625719SSM 625720SSM 625721SSM 625730SSM 625788SSM 625789SSM 625790SSM 625791SSM 625792SSM 625793SSM 625794SSM 625795SSM 625796SSM 625797SSM 625798SSM 625799
cut Line (metres)
900 400 400 800 800 700 700 700 nil nil 750 800 800 800 850 400 700 700 800 800 100 800 800 800 800 400 nil 200 300 550 500 500 400 nil 300 200 nil 800 4001200 80012001300 400 450 900 4001050 550
T*t*le fi (cont' d)
Claim Number
SSM 625800SSM 625801SSM 625802SSM 625803SSM 625804SSM 625805SSM 625806SSM 625807SSM 625808SSM 625809SSM 625810SSM 625811SSM 625812SSM 625813SSM 625814SSM 625815SSM 625816SSM 625817SSM 625818
Cut Line (metres)
3007007259509001150800700
120050
350500500750800400100100150
Claim Number
SSM 625819 SSM 625820 SSM 625821 SSM 625822 SSM 625823 SSM 625824 SSM 625825 SSM 625826 SSM 625830 SSM 625831 SSM 625832 SSM 625833 SSM 625834 SSM 625835 SSM 626737 SSM 626738 SSM 1172594 TB 1097120 TB 1097121
Cut Line (metres)
600600400nilnil600750750200
105012001175650500800800800nil50
DUPLICATE42C12NE0006 2.16056 BROTHERS 030
1.5 SUMMARY OF WORK PERFORMED
Vytyl Exploration Services (2035 Montrose Place, Thunder Bay, Ontario, P7J 1A4) was contracted for the linecutting. There was a total of 28.7km of cut/surveyed line and 146km cut line that was established. The baseline trends east/west with cross lines in a north/south orientation. The line spacing is 200m with a station interval of 25m. The stations are identified with pickets, and metal tags with the inscribed grid coordinate were stapled to them. Although there was a total of 174.7km of line that was established, only 133.7km of the grid was covered by the geological survey.
The geological mapping portion of the 1994 exploration programme extended from June 16th to August 28th (inclusive). Napping was conducted at a scale of 1:2,500 along and between the grid lines. Features were located using hip chain and compass as well as GPS (Global Positioning System).
The geological mapping was performed by S. Beauchamp, R. Lemaitre, B. Nelson and G. Shevchenko, with assistance provided by D. Goyette, C. Green, Z. Hunt, A. Nace and H. Sellers. The digitizing and Autocad drafting for this report was carried out by C. Green and C. Davis. The mapping program was supervised by G. Shevchenko (c/o Placer Dome Canada Limited, Box 960, Timmins, Ontario, P4N 7H1).
W.A. Barclay Exploration Services Ltd. (23 Grenadier Rd., Toronto, Ontario, M6R 1R1) was contracted between June 16th and July 15th ( inclusive) to conduct structural mapping and interpretation.
The following table lists the claims and amount of cut line which were actually covered by the geological survey.
Table f is List of Claims Worked
Claim Number cut Line(metres)
Claim Number Cut Line (metres)
SSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSM
5425885425895425905425916077446077456077466077476077486077496077656077666077676077686077696077706077716077726077876077886077896077906078656078666078676078686078696078706078716078726078736078746078786O7879607880
6501100900650350550650800800800600120012001200800800800400400750700400nilnil375800800800700900900450300
15OO1300
SSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSMSSM
607881607882607883607884607943607946607947607948607960607961607962607963607964607965607966607967607968607969607970607972607973625556625557625585625586625587625588625589625591625592625593625594625595625597625598
1650nilnilnilnil675600nil7501200120080015007007509001000875450800600nilnil100011503004008008008008008004006OO800
Table (cont'd)
Claim number
SSM 625599SSM 625600SSH 625602SSM 625603SSN 625604SSN 625605SSH 625606SSN 625607SSN 625608SSN 625609SSH 625616SSH 625617SSN 625618SSH 625619SSH 625621SSH 625622SSH 625623SSH 625629SSH 625630SSN 625631SSN 625632SSH 625633SSH 625652SSH 625653SSH 625658SSH 625659SSH 625660SSH 625661SSH 625664SSH 625665SSH 625666SSH 625667SSH 625668SSH 625669SSH 625670SSH 625671SSH 625672SSH 625673SSH 625674SSH 625675SSH 625676SSH 625677SSH 625678SSH 625679SSH 625680SSH 625681SSN 625682SSH 625683SSH 625684
Cut Line (metres)
700675400800 1000 1200800 1000 1150 1100800450700225200200800
1100250600800nil 1325600
1125 1200 1050450nil1050
75950700700600350400250325600250550800 1100 1200 1200 1200550800
Claim number
SSH 625685SSN 625686SSN 625687SSH 625688SSH 625689SSH 625690SSH 625691SSH 625692SSH 625693SSH 625694SSH 625695SSH 625696SSH 625697SSH 625698SSH 625699SSH 625700SSH 625701SSH 625702SSH 625704SSH 625705SSH 625706SSH 625707SSH 625708SSH 625709SSH 625710SSH 625711SSH 625712SSH 625713SSH 625714SSH 625715SSH 625716SSH 625717SSH 625718SSH 625719SSH 625720SSH 625721SSH 625730SSH 625788SSH 625789SSH 625790SSH 625791SSH 625792SSH 625793SSH 625794SSH 625795SSH 625796SSH 625797SSH 625798SSH 625799
cut Line (metres)
900400400800800700700700nil nil 750 800 800 800 850 400 700 700 800 800 100 800 800 800 800 400 nil 200 300 550 500 500 400 nil 300 200 nil 800 400
1200 80012001300 400 450 900 4001050 550
e fi (cont'd)
Claim number
SSM 625800SSN 625801SSN 625802SSN 625803SSN 625804SSN 625805SSN 625806SSN 625807SSN 625808SSN 625809SSN 625810SSN 625811SSN 625812SSN 625813SSN 625814SSN 625815SSN 625816SSN 625817SSN 625818
Cut Line (metres)
3007007259509001150800700
120050
350500500750800400100100150
Claim Number
SSN 625819 SSN 625820 SSN 625821 SSN 625822 SSN 625823 SSN 625824 SSN 625825 SSN 625826 SSN 625830 SSN 625831 SSN 625832 SSN 625833 SSN 625834 SSN 625835 SSN 626737 SSN 626738 SSN 1172594 TB 1097120 TB 1097121
cut Line (metres)
600600400nilnil600750750200105012001175650500800800800nil50
Ministry ofNorthern Developmentand Mines
Report of Work Conducted After Reccyc';r - Claim
Transaction Number
OntaTio Minin Act^ersonal information collected on this form is obtained under the authority of the Mining Act. This information will be used for correspondence Questions about (his collection should be directed to the Provincial Manager. Mining Lands. Ministry of Northern Development and Mines. Fourth Floor. 159 Cedar Street. Sudbury. Ontario. P3E 6A5. telephone (705) 670-7264.
instructions: - Please type or print and submit in duplicate.- Refer to the Mining Act and Regulations for ree
Recorder.- A separate copy of this form must be complete- Technical reports and maps must accompany t- A sketch, showing the claims the work is assig
. 1 C O 56
42C12NE0008 216056 BROTHERS 900Recorded Holders) FOR: LAC MINERALS LTD.
Address2 BOUSQUET RD. , ROUTE 395 PREISSAC, QUEBEC JOY 2EO
MMng Division THUNDER BAY
Work From: JuflC 1/94•fc-j-, ,-, , . * 1 t^enonnoo
Township/Area B6MBY, BROTHERS, LABERGE
Client NO.155133
Telephone No. 819-759-3681
M or 6 Plan No. SMrW, G3172, G3174
TO: Sept 15/94
Work Performed (Check One Work Group Only)! WorkGroup
Geotechnical Survey
Physical Work. Including Drilling
Rehabilitation
Other Authorized Work
Assays
Assignment from Reserve
Type
GEOLOGICAL SURVEY
nCCEIVED
jUN ' i9;b
/iMNG LANOa BRANCH
Total Assessment Work Claimed on the Attached Statement of Coststote: The Minister may reject for assessment work credit all or part of the assessment work submitted if the recorded
holder cannot verify expenditures claimed in the statement of costs within 30 days of a request for verification.
^ersons and Survey Company Who Performed the Work (Give Name and Address of Author of Report)Name
Glenn Shevchenko
Vytyl Exploration Services
Barclay Exploration Services
Address
c/o Placer Dome Canada, Box 960, Timmins, Ont.P4N
2035 Montrose Place f Thunder Bay ̂ Ont* P7J 1A4
i 23 Grenadier Rd,, Toronto, Ont. M6R 1R1
7HJ
ittach a schedule H necessary)
•ertification of Beneficial Interest * See Note No. 1 on reverse sidel certify that at the time Hw work was performed, the claims covered in this work report war* recorded in the currant hoUefs name or held under a beneficial interest by the currant recorded holder.
MAY 24/95(Recorded Holder or Agent (Signature)
LAND MANAGEREJertlf (cation off Work Reportl certify that l have a personal knowledge of the facts set forth in this Work report, having performed the work or witnessed same during and/or after its completion and annexed report is true.
AUL BURCHELL, C/O PLACER DOME CANADA LTD.BOX 960, TIMMINS, ONT. p4N 7H1
itaponeNo. 05-267-5400 MAY 24/95
Office Use Only
41(0*911
Ontario
Ministry OtNorthern Developmentand Mines
Mmislere du Developpement du Nord ei des mines
Statement of Costs for Asse^ ne* it CreditEtat des couts aux fins du credit devaluation
Mining Act/Loi sur les mines
Transaction No /N" de transaction
Personal information collected on this form is obtained under the authority of the Mining Act. This information will be used to maintain a record and ongoing status of the mining claimfs). Questions about this collection should be directed to the Provincial Manager. Minings Lands. Ministry of Northern Development and Mines. 4lh Floor. 159 Cedar Street. Sudbury. Ontario P3E 6A5. telephone (70S) 670-7264.
Les renseignements personnels contenus dans la presente formule sont recueillis en vertu de la Loi sur les mines et serviront d tenir A jour un registre des concessions mimeres Adresser tcuie question sur la coiiece de ces renseignements au chef provincial des terrains miniers. m- nslere du Developpement du Nord et des Mines. 159. rue Cedar. 4e etage. Sudbury (Ontario) P3E 6A5. telephone (705) 670-7264
1. Direct Costs/Couts directs
Type
Wages Sateirm
Contractor's and Consultant's Fees Droits de (•entrepreneur et de I'expert- conseil
Supplies Used Foumituras utilisees
Equipment Rental Location de materiel
Description
Labour Main-d'oeuvreField Supervision Supervision sur le terrain
Type W . A . BAKCliASXPL. SVCS
fYTYL EXPL.SVC
Type FIELD
di?S RENTAL
COMPUTER RENT.
RADIOS
Amount Montan!
40141
L8792
7514
rt 811-
860Q
^L
Total Direct Costs Total des couts directs
Totals ' Total global
58933
i
68325
i
8600
11810
47668.
2. Indirect Costs/Couts indirects* * Note: When claiming Rehabilitation work Indirect costs are not
allowable as assessment workPour le remboursement des travaux de rehabilitation, les couts indirects ne sont pas admissibles en tant que Iravaux devaluation.
Type
Transportation Transport
Food and Lodging Nourriture et hebergementMobilization and Demobilization Mobilisation et demobilisation
DescriptionAmount Montan!
VEHICLE EXPENdE 4020
TRAVEL 7420
16469
Sub Total of Indirect Costs Total partiel des couts indirects
Amount Allowable (not greater than 20H of Direct Costs) Montan! admissible (n'excedant pas 20 H des couts directs)Total Value of Assessment Credit Valeur totale du credit (ToM of Direct end AHowabta d evaluation Indlnct costal ITatil dM null dlradi
Totals Total global
11440
16469
27909
175577
•(In
Note: The recorded holder will be required to verify expenditures claimed in this statement of costs within 30 days of a request for verification. If verification is not made, the Minister may reject for assessment work all or pan of the assessment work submitted.
Note : Le tituiaire enregistre sera tenu de verifier tes depenses demandees dans le present etat des couts dans tes 30 jours suivant une demande a eel effet Si la verification n'est pas effectuee. le ministre peut rejeter tout ou une partie des travaux devaluation presentes
Filing Discounts
1 . Work filed within two years of completion is claimed at the above Total Value of Assessment Credit.
of
2. Work filed three, four or five years after completion is claimed at 504b of the above Total Value of Assessment Credit. See calculations below:
Total Value of Assessment Credit Total Assessment Claimed
x 0.50
-,- ^i i. *i^i i *
RLCFIVEDRemises pour depot
i Les travaux deposes dans les deux ans. suivantrembourses a 100 "to de la vateur totale susrrieHtonnee du credit d'S-'.-
f • -. •' 5
2. Les travaux deposes trois. quatre ou cinq ans apres leur achievement sont rembourses a 50 H de la valeur totale du credit d'evaluatkm susmentionne. Voir les calculs ci-dessous.
l Valeur totale du credit devaluationl
Evaluation totale demandee
x 0.50
Certification Verifying Statement of Costs Attestation de I'etat des couts
he'eby certify:hat the amounts shown are as accurate as possible and these costs vere incurred while conducting assessment work on the lands shown jn trie accompanying Report of Work form.
-iat as Land Manager(Recorded Holder. Agent. Position m Company)
o make this certification
J'atteste par la presenteque les montants indiques sont le plus exact possible et que ces depenses ont etc engagees pour effectuer les travaux devaluation sur les terrains indiques dans la formule de rapport de travail ci-jomt
l am authorized Et qu'a litre de. je suis autonseH tuiaire enreg sire, wese-ian:. pos'e occuce dans 'a compagniei
a faire cette attestation.
; Signature ;Oate
l May 24/95
Nota Dans cette formule lorsqu'il des gne des persc"es. le rnascul n esi jTihse au se-'S neutre
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Page Ne. ir
06/06/1995
Work Report
NMber for
Reserve
l l
o f*IAMIA
Total ***
CLAIM NUMBER
Tl 1122904 Tl 1122905 IB 1122906Tt 1122907 TB 1164907 TB 116490ft TB 1164909 Tl 1164910 TB 1164911 TB 1164912 TB 1164913 TB 1164914 Tl 1164915
SW 1172954
SCHEDULEREPM
I OF WOMC CONDUCTED AFTER RECORDING CLAIM
OfC
lalN
UhfU1
Value ofAM
MM
entUork Don*
en thla dale)
0.00 0.00 0.00 0.00 0.00 O.DO 0.00 0.00 0.00 0.00 0.00 0.00 0.00
1060.00
175577.00
Value Applied to thie
cut*
400.00400.00400.00400.00400.00400.00400.00400.00400.00400.00400.00400.00400.00
175*77.00
ValueAaalgned
fromthta Ctain
0.000.000.000.000.000.000.000.000.000.000.000.000.00
U66M.OO
Reserve:W
ork to beClaimed it
a Future Date
0.000.000.000.000.000.00O.OD0.000.000.000.000.000.000.00
0.00
IAtt XW
,
OntarioMinistry ofNorthern Developmentand Mines
Ministere duDeveloppement du Nord et des Mines
July 12, 1995
Mining Recorder Ministry of Northern Development 6 Mines 435 Janes Street South Suite B003Thunder Bay, Ontario P7A 6E3
Dear Mr. Weirmeir:
Geoscience Approvals Office 933 Ransey Lake Road 6th Floor Sudbury, Ontario P3E 6B5
Telephone: Fax:
(705) 670-5853 (705) 670-5863
Our File: 2.16056 Transaction #: W9540.00132
SUBJECT: PPROVAL OP ASSES WORK CREDITS ON MINING CLAIMS 542588 ET AL. IN BROTHER8/LABBROE TOWNSHIPS
Assessment work credits have been approved as outlined on the original report of work forms for this submission. The credits have been approved under Section 12, Geology, of the Mining Act Regulations.
The approval date is July 12, 1995. Please indicate this approval on the claim record sheets.
If you have any questions regarding this correspondence, please contact Bruce Gates at (705) 670-5856.
Yours sincerely.
Ron C. GashinskiSenior Manager, Mining Lands Section Mining and Land Management Branch Mines and Minerals Division
BIG/jn
cc: Resident GeologistThunder Bay, Ontario
Assessment Files Library Sudbury, Ontario
REFERENCES
AREAS WITHDRAWN FROM DISPOSITION
M.R.O. - MINING RIGHTS ONLY
S.R.O. - SURFACE RIGHTS ONLY
M.-r S. - MINING AND SURFACE RIGHTS
DMoription Order No D*t* O upon t ion File
(RJ) CROWN RFSFRVF Suiface Righls Only Mie I8854G.
/oToN Suiface 8 Mining Rights withdrawn f tom staking.v—'Section 43 Mining Act R 5.0.19^0 Dated Sept. P5/79
File 188546 Oidei No WI4/79. Pic Mobeit Indian Band(R*} Surface Rights Only withdrawn from staking. ^^ Sec .46 Mining Act RS.0.1980. Ord.r No. W-2/81
Dated feb. 17/81 file 188546. Landfill Site.
/o7\ Surface Rights Only withdrawn from staking. VH* s ec 36 Winino Act R.S 0.1980 Order No. W-6/82.
Dated 5/4/62. File 188546. Wait. Disposal Site.
FLOODING RIGHTS ON WHITF RIVER AND WHI l E LAM TO CONTOUR ELEVATION lOBO TO ONTARIO HfDRO.
ALL MINING CLAIMS ALONS WHITE RIVER AND CONNECTING LAKfS ARE SUBJFCT 10 SEC. 41 OF THE MININC ACT, R.S.O. 19 f O FILE 115890
WHITE LAKE (S.PT) G-623
" * ~ *
'6861
test
,88M
1629
l , SSM
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NOTICE:The information that appears on this map has been compiled from various sources and accuracy is not guaranteed l hose wishing to stake MINING CL AIMS should consult with the MINING RFCORDr'R. Minnlry of Northern Development and Mines, for additional information on the status of the lands shown lieruoii
'l 6251 '625715
J689707 |6?570C S*M~ "
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- ——— L ——— L ——— l ——— -J---1-~HO.66.4
OSKABUKUTA LAKE 6-3775
LEGENDHIGHWAY AND ROUTE NoOTHER ROADSTRAILS -SURVEYED LINES
TOWNSHIPS BASE LINES ETCLOTS MININC, CLAIMS PARCELS, ETC
UNSURVEYED LINESLOT LINESPARCEL BOUNDARYMINING CI AIMS ETC
RAILWAY AND RIGHT OF WAY f
UTILITY LINES -* NON PERENNIAL STREAM FLOODING OR FLOODING RIGHTS i: SUBDIVISION OR COMPOSITE PLAN RESERVATIONS ORIGINAL SHORELINE MARSH OR MUSKEG MINESTRAVERSE MONUMENT INDIAN RESERVE
DISPOSITION OF CROWN LANDS
TYPE OF DOCUMENTPATENT SURFACE A MINING RIGHTS
.SURFACE RIGHTSONLYMINING RIGHTSONLY
LEASE, SURFACE * MINING RIGHTS. " .SURFACE RIGHTSONLY . ..
MINING RIGHTSONLY
ir OCCUPAflON ..—........
SYMBOL
RESERVATION .. . . .CANCELLED ..... . . . . .SANO ft GRAVEL .-... ....,. .. .. . . .
LAND USE PERIMTS FOR COMMERCIAL TOURISM, OUTPOST CAMPSNOTE MININU RIGHTS IN PARCELS PATENTED PRIOR TO MAY 6
1S13 VESTED IN ORIGINAL PATENTEE BY THE PUBLIC LANDS ATT RSO 1970 CHAP 3.0 SEC 83 SU.6EC 1
(J)/ V
SCALE 1 INCH 40 CHAINS
1000 ,-OQO 4000 6000 8000
O iOOW t T R l :,
1000l l KMI
200012 KM}
TOWNSHIP fc a ]|U (II)
LABERGEM N.R ADMINISTRATIVE DISTRICT
WAWAMINING DIVISION
SAULT STE. MARIELAND TITLES/ REGISTRY DIVISION
THUNDER BAY
MmiStryof Land
Natural Management
Resources BranchOntario
D '" AUGUST 1984
hi SwvUw FEB. O* /M.
Number
G-317442C1 200
REFERENCESA^BAl WITHDRAWN FROM DISPOSITION
M.H.O. - MINING RIGHTS ONLY
B.R.O. - SURFACE RIGHTS ONLY
M.+1. - MINING AND SURFACE RIGHTS
Onto No. Oat* DtafMiitkm
WABIKOBA LAKE 6-620 WHITE LAKE (S.PT.) G-623
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THE INFORMATION THAT APPEARS ON THIS MAP HAS BEEN COMPILED FROM VARIOUS SOURCES, AND ACCURACY IS NOT GUARANTEED THOSE WISHING TO STAKE MIN ING CLAIMS SHOULD CON SULT WITH THE MINING RECORDER MINISTRY OF NORTHERN DEVELOP MENT AND MINES, FOR AD DITIONAL INFORMATION ON THE STATUS OF THE LANDS SHOWN HEREON
HERRICK LAKE
HIGHWAY AND ROUTE No OTHER ROADS TRAILSSURVEYED LINES
TOWNSHIPS, BASE LINES, ETCLOTS. MINING CLAIMS PARCELS. ETC
UNSURVEYED LINESLOT LINESPARCEL BOUNDARYMINING CLAIMS ETC
RAILWAY AND RIGHT OF WAY UTILITY LINES NON-PERENNIAL STREAM FLOODING OH FLOODING RIGHTS SUBDIVISION OR COMPOSITE PLAN RESERVATIONS ORIGINAL SHORELINE MARSH OR MUSKEGMINESTRAVERSE MONUMENT
DISPOSITION OF CROWN LANDS
TYPE OF DOCUMENT .PATENT. SURFACE ft MINING RIGHTS
" . SURFACE RIGHTS ONl Y....." . M INING RIGHTSONLY ,. .... .
LEASE. SURFACE ft MINING RIGHTS.. " .SURFACE RIGHTS ONLY.. . .
MINING RIGHTSONLY.. . ...LICENCE OF OCCUPATION ...-.. ....ORDER-IN-COUNCIL .... .... .. ....RESf-RVATION .. .
"CTtNCtLLED . ..,. .. .. .
SYMBOL
d
QTOC
SAND 8. GRAV-FL ........ . .. . .... ..(J)LAND USE PERMITS FOR COMMERCIAL TDURI3M.OUTP06T CAMP* V
NOTE MINING NIUHTS IN PAHCtLS PATENTED PRIOR 'O MAY 6, 1*13 VESTfO IN OHK5INAI PATtNItt B* Tllf PUBLIC
A( I H b O 1W/U C HAK JBO ilt 6J *UB6fcC 1
SCALt l INCH - 40 CHAINS
i finn /ooo 4OOO 6OOO •000
1000l l KM.
2030(2 KM)
;.0'-BROTHERSM.N R. ADMINISTRATIVE DISTRICT
TERRACE BAY / WAWAMININt OIVISIOK
SAULT STE.MARIE/THUNDER BAlLAND TITLES/ REGISTRY DIVISION
THUNDER BAYMmistryof LandNatural ManagementResources Branch
AUGUST, 1964
G-3172
210
Gaby Lake
. A lder
fi M
Lake
White
Lake
Te da Flora Lake
V ursery
- ^ ~-- : ^ " . "UT ~ ̂ gjT^~ . fc'-^S: ^——z"
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Spangle Lake
Fearless Lake
i a A: e
ck
-^ L akeLake
ZaArc Oskabukuta Lake
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160
D-::~ : 505
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G:\acaddwgs\505\94_maps\wrwork.dlug
42C12NEOMK 2.1BO56 BROTOBIS 230
O 1000 2000 m
SCALE BAR
i i 'i '..^-————^——4——-f———J JTB 1074781
CEDAR LAKE PLUTON
9a
5392000N
UPPERANOMALOUSHORIZON
5391500N
60 /GAR
B.L CUT TO HERE
B.L. CHAINED TO HERE
5391OOON
-^;:fe^•A jL.fi l l
2 (Minor 3)2 (Minor 3)
2 (Minor 3)
HEMLO FAULT
\
\
5390500N
5390000N
UJo oLOr- ooLO
Ldo o o oo ooLO
LUo oLO0000LO
LJo ooCD 00LO
LEGEND
INTRUSIVE ROCKS
Late Mafic Dike (Diabase): approx equal proportion* of plagioclase and pyroxene
Earlj Mane Dike. Sill: foliated, deformed gabbro, amphibolite or biotite amphibolite
Felaio to Intermediate Intrusive Rock*9a Granite: ^X mafic, ^H quarts, may be porphyritic9b Cranodiorite/DioHte: ^X mafic, >fiX quartz9d Syenite: ^X mafic, ^X quartz9e Pegmatite Dike: ooarae to very coarae grained feldspar i quart* i
mica9f Aplite Dike: quarts It feldapar, no mafioa 9g Felaio Dike: Oh Grey Feldspar Porphyry: white feldspar pbenooryata act in a grey
matrix 91 Pink Feldapar Porphyry: pink feldapar phenocryst* aat in a
pink/grey/wbita matrix 9J Quartz-Feldspar Porphyry: 9k Quartz Porphyry:
Pukaskwa Gneiaaio Complex: Hornblende-biotite bearingTonalite/Granodiorite/quartz Diorite, may be plagioclase porphyritic
META8EDIMENTARY ROCKS
Arenite: generally ^X mafic, quartz ia the main constituent (ie: ^OX), may contain feldspar
Arkosic Wacke6a Feldsper-Quarts-Biotite Gneiss: generally feldspar dominant.
^OX quartz, O6X biotite,Ab Feldspar-Qnartz-Biotite-Amphibole Gneiss: generally feldapar
dominant, ^OX quartz, O6X mafic— Quar t8 — ̂ p
quanir ̂ i BXWaoke
6a BloUte-Feldapar-Quarta Gneiss: generally feldspar dominant.^OX quarts. MoX biotite
6b Biotite-Amphibole-Feldspar Quarts Gneiss: generally feldspardominant, ^OX quartz, M69C mafic
6c Amphibole-Feldspar-quartx Gneiss: generally feldapar dominant, quartz, >16X amphibole
UETAVOLCANIC ROCKS
Felaio Voloanio Rooks: quart*, ^X mafio4a Felsic Fragmental: white feldapar pbenoa set in aphanitic white
matrix
Intermediate Voloanio Rooka: quarts, 6 to 60X mafio 3a Massive Tuff/Flow:3b Crystal Tuff: containa quartz t feldapar phenocryst* 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quartz-feldspar flattened
Mafic Volcanic Rocks: generally no quarts and approx equal proportions ofmafic and plagioclase
2a Massive Flow: 2b Pillowed Flow:2o Feldapar-Amphibolite: ^OX amphibole, feldspar 2d Quartz-Ampbibolite: ^OX amphibole, quartz 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs in white
to greenish white lenses
ROCKS OF UNKNOWN ORIGIN
QZSS (Q8S) Quartz-Serioite SchistQE88 (qSS) Quartz eye Sericite SchistQEP Quartz-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
CLSE TA SI
PR PY
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KF EP BI
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMP QTZ FQV
BND BRX CRN PEG AFG MSV FOI.
GarnetAmphiboleQuartsFeldspar-Quarts vein
TEXTURES
BandedBrecciatedCrenulatedPegmatiticAphanitic to fine grainedMassiveFoliated
MAG MagnetiteBIO BioliteFELD Feldeper
PPH XEN PPB COR FRG DET SCH
..M rltic Xenolfthic Porphytoblaatio Coarse grained Fragmental Detrital Schistose
J) j
Efl[ E *j U2
STRUCTURAL SYMBOLSSmall Scale FI Fold Minor Fold Axis F2 11 -Fold Axis F3 M*Fold Axis F2 S-Fold Axis F3 S-Fold Axis F2 W-Fold Axis F3 W-Fold Axis ?2 Z-Fold Axia F3 Z-Fold Axis
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
J CLAIMPOST
) DUMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
GEOLOGICAL CONTACT
LITHOLOGICAL UNIT
ROAD
TRAIL
FOLD AXIS
FAULT
CLIFF
L?84E GRID LINE LABEL
"j GRID STATION (100m interval)
l ] BASK OF SLOPE (may be swamp boundary)
XXX X X BEAVER DAM
BeddingBreccia Clasta82 FoliationS3 Foliation81/80 Compositional BandingD3 Fracture
89
6
KEY TO MAP SHEETS
4JC1240
D PLACER DOME OMADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP(SHEET 1)
DATF: April, 1995
SCALE: 1 :2500
ORIG BY: G S DRAWN BY: C CD
NTS REF:42 C /12
DWG.NO. 6
FIEE: WRGL01.DWG C \WRIVER\ACADDWCS\GEOL94\REPORT
" ' R ust LakeQuartz Porphyry
9k
CEDAR LAKE PLUTON
5392000N
I3cU
9600, N
-3391 SOON
6a /GAR
_ —^
3d6a~/GAR\ \L23200 E 9025 N MAIN GRID
L23200 E BL 9000 N EGG GRID\ \
\ \
\ \X A 5391000N
X \\ \\ x
\ \
2 (minor 2b)
5390500N
11 V
l
LEGEND
INTRUSIVE ROCKS
Late Mafia Dike (Diabase): approx equal proportion* of plagioclase and pyroxene
Early Mafic Dike, Sill: foliated, deformed gabbro, amphibolite or biotite amphibolite
Felite to Intermediate Intnuive Rock*9a Granite: ^H mafic, ^X quarts, may be porphyriticOb Granodiorite/Dlorite: ^X mafic, ^35 quartzOd Syenite: ^X mafic, c6X quart*Oe Pegmatite Dike; coarse to very coarse grained feldspar i quartz ±
micaOf Aplite Dike: quartz * feldspar, no mafics Og Felsic Dike: Ob Grey Feldspar Porphyry: white feldspar phenocryst* set lo a grey
matrix 01 Pink Feldspar Porphyry: pink feldspar phenocryst* set in a
pink/grey/wbite matrix Oj Quarts-Feldspar Porphyry: Ok Quartz Porphyry:
Pukaskwa Gneissic Complex: Hornblende-biotlte bearingTonalite/Granodiorlte/Quarts Diorite, may be plagioclase porphyritic
METABEDIMENTARY ROCKS
Arenite: generally ^X mafic, quarts i* the main constituent (ie: ^OX), may contain feldspar
Arkosic Wacke0a Feldspar-Quartz-Biotite Gneiss: generally feldspar dominant,
^0* quartz, ^6Z biotite, Ob Fftldapar-QiiBrtz-Rtolitu-Amphibole Gneiss- generally feldspar
dominant, KMft quart*, 41ft* OMlfcBo Feldspar-Quarti-Amphibole Gnelaa: generally feldspar dominant,
<605{ quarts, <1B% amphibole
Wacke6a Biotite-Feldapar-Quartz Gneiss: generally feldspar dominant,
^60* quarts, M5X biotite 6b Biotite-Ampbibole-Feldipar Quartz Gneiss: generally feldspar
dominant, ^OX quartz, > ^&% mafic60 Amphibole-Feldspar-Quartz Gneiss: generally feldspar dominant,
quarts, J-16X amphibole
METAVOLCANIC ROCKS
Felsic Volcanic Rooks: quartz, ^X mafic4a Felsic Fragmental: white feldspar phenoa set in aphanitic white
matrix
Intermediate Volcanic Rocks: quartz, fi to BOX mafic 9a Massive Tuff/Flow:3b Crystal Tuff: contains quarts ? feldspar phenocryst^ 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quartz-feldspar flattened
Mafic Volcanic Rooks: generally no quartz and approx equal proportions ofmafic and plagioclase
2a Massive Flow: 2b Pillowed Flow:2c Feldspar-Amphibolite: ^OX amphibole, feldspar 2d Quartz-Amphibolite: ^OX amphibole, quartz 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs In white
to greenish white lenses
ROCKS OF UNKNOWN ORIGIN
QZSS (QS8) Quartz-Serioite SchistQES8 (QE8) Quartz eye Sericite SchistQEP Quartz-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
CLSE TA SI
PRpy
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KF IP BI
MINERALIZATION
SI
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMP QTZ FQV
BND BRX CRN PEG AFG MSV FOL
GarnetAmphiboleQuartzFeldspar-Quartz vein
TEXTURES
BandedBrecciatedGranulatedPegmatiticAphanitic to fine grainedMassiveFoliated
MAGBIOFELD
PPH XEN PPB CGR FRG DET SCH
MagnetiteBioliteFeldspar
PorphyriticXenolfthicPorphytAblMUoCoarse grained Fragmental Detrital Schistose
STRUCTURAL SYMBOLS
Small Scale FI Fold Minor Fold Axis F2 M-Fold Axis F3 M-Fold Axis F2 8-Fold Axis
( jfc F3 8-Fold Axis F2 W-Fold Axis F3 W-Fold Axis F2 Z-Fold Axis F3 Z-Fold Axis
BeddingBreccia Clast*82 FoliationS3 FoliationSI/SO Compositional BandingD3 Fracture
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
CLAIMPOST
DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
——— GEOLOGICAL CONTACT
C'j LITHOLOGIC AL UNIT
- : ROAD
....x TRAIL
* FOLD AXIS
^ FAULT
'"""""r CLIFF
L284E GRID LINE
j GRID STATION (100m interval)
_J j BASE OF SI.OPE (may be nwamp boundary)
VO ** BEAVER DAM
4
89
6
KEY TO MAP SHEETS
250
D PLACER DOME CANADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP(SHEET 2)
DATE: April, 1995
SCALE: 1 : 2500
ORIG BY: G S DRAWN BY: CCD
NTS REE.42 C/12
DWG.NO. 7
EI LE: WRGL02.DWG G \WRIVER\ACADDWGS\GEOU94\REPORT
gb/MAG
95/MAG
6a /GAR
f- rrr*^f
LLOWYELAKES 5390500N
l
LEGEND
INTRUSIVE BOCKS
Late Mafic Dike (Diabase): approx equal proportions of plagioclase and pyroxene
Early Mafic Dike. Sill: foliated, deformed fabbro, amphibolite or biotite amphibolite
Felsic bo Intermediate Intrusive Rocks9a Granite: <5% mafic, >5yt quartz, may be porphyritic0b Granodiorite/Diorite: >SX mafic, >5% quartz9d Syenite: <5% mafic, <5X quartz9* Pegmatite Dike: coarse to very coarse (rained feldspar ± quartz ±
mica9f aplite Dike: quartz le feldspar, no mafica 9g Felaic Dike: flh Grey Feldspar Porphyry: white feldspar phenocrysta set m a frey
matrix 91 Pink Feldspar Porphyry: pink feldspar phenocrysta set in a
pink/frey/white matrix Oj Quartz-Feldspar Porphyry: 9k Quartz Porphyry:
Pukaskwa Gneissic Complex: Hornblende—biotite bearingTonalite/Granodiorite/Quartz Diorite, may be plagioclase porphyritic
METASEDIMENTARY ROCKS
Arenite: fenerally OX mafic, quartz is the main constituent (le: >5QX'), may contain, feldspar
Arkosic Wacke6a Feldspar—Quartz-Biotite Gneiss: generally feldspar dominant,
<SOX quartz. <15% biotite. Sb Feldspar-Quarta-Biotite-Ampnibole Gneiss: generally feldspar
dominant, <50% quartz. -CIS* mafic flc Feldspar—Quartz—Amphibole Gneiss: generally feldspar dominant,
<50% quartz, •C 1535 amphibole
Wacke 5a
Sb
Se
Biotite—Feldspar—Quartz Gneiss: generally feldspar dominant.<50% quartz. M5X biotiteBiotite-Amphibole-Feldapar Quartz Gneiss: generally feldspardominant, ^03! quartz, 3*1535 maficAmphibole-Feldspar-Quartz Gneiss: generally feldspar dominant,<5OX quartz, >15X amphibole
METAVOLCANIC ROCKS
Felsic Volcanic Rocks: quartz. ^X mafic4a Felsic Fragmental: white feldspar phenos set in aphanitic white
matrix
Intermediate Volcanic Rocks: quartz. 5 to 503 mafic 3a Massive Tuff/Flow:3b Crystal Tuff: contains quartz ? feldspar phenocrysta 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quartz -feldspar flattened
Mafic Volcanic Rocks: generally no quartz and approx equal proportions ofmafic and plagioclase
2a Massive Flow: 2b Pillowed Flow:2c Feldspar- Amphibolite: ^OX amphibole, feldspar 2d Quartz— Amphibolite: >70% amphibole, quartz 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs in white
to greenish white lenses
ROCKS OF UNKNOWN ORIGIN
QZSS (QSS) Quartz-Sericite SchistQESS (QES) Quartz-eye Sericite SchistQEP Quartz-eye PorphyryQB Weakly Sericitic Felsic Volcanic
ALTERATION
CL SE TA SI
PR PY
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KF EP BI
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
GAR AMP QTZ FQV
END BEX CRN PEG AFG MSV FOL
GarnetAmphiboleQuartzFeldspar-Quartz vein
QUALIFYING MATERIALS
MAGmoFELD
TEXTURES
Banded PPHBrecciated KENCrenulated PPBPegmatitic CGEAphanitic to fine grained FRGMassive DETFoliated SCH
MagnetiteBiotiteFeldspar
PorphyriticXenolithicPorphyto blasticCoarse grainedFragmentalDetritalSchistose
STRUCTURAL SYMBOLS
Small Scale FI Fold 3——^ Minor Fold Axis
J) fr F2 M-Fold Axis F3 M-Fold Axis F2 S-Fold Axis F3 S-Fold Axis F2 W-Fold Axis F3 W-Fold Axis F2 Z-Fold Axis F3 Z-Fold Axis
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
CLaJMPOST
DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
GEOLOGICAL CONTACT
UTHOLOGICAL UNIT
ROAD
TRAIL
FOLD AXE
FAULT
^" CLIFF
L284E GBn)
GRID STATION (100m interval)
BASE OF SLOPE (may be swamp boundary)
BEAVER DAM
Bedding Breccia Claats52 Foliation53 FoliationS l/SO Compositional Banding
D3 Fracture
3'//////A
89
KEY TO MAP SHEETS
42012180* 2.16098 BROTHBra 260
D PLACER DOME CANADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP ;(SHEET 3)
DATE: April, 1995
SCALE: 1 :2500
ORiG BY: GS DRAWN BY: CCD
NTS RER42 C/12
DWG.NO. 8
FILE: WRGL03.DWG G:\WRIVER\ACAOOWGS\GEOL34\REPORT
LITTLETERSP
Qa/PPHKELA
Sa/GAR
N \ 6Q/GAR\ \\ \
3 (minor 2d) \
Tog K. 62579*Toj 43- 925799To? J*- 523608
YELLOW BIRCH Sa.c/GARSc/GAR W iLAKE
HEMLO FAULTvy\ x./"1 oo *^r\ i^ v-^ v-T^O^ *^/-* Lo v^o L-O v.O v^n un vy-% ^r\ v.n ^o *v^ c/^ ^r* vy^
HEMLO FAULT
RIVERWHITE
LEGEND
DTTRUSIVE ROCKS
Late Mafic Dike (Diabase): approx equal proportions of plagioclase and
Early Mafic Dike. Sill: foliated, deformed fabbro, amphibolite or biotite amphibolite
Felsic to Intermediate Intrusive Rocks0a Granite: OX mafic, ^11 quartz, may be porphyritic9b Granodiorite/Diorite: ^H mafic, >S% quartz9d Syenite: <5X mafic, <S% quartz9* Pegmatite Dike: coarse to Tery coarse grained feldspar ± quartz ±
mica9f Aplite Dike: quartz tt feldspar, no mafics 9g Felsic Dike: 0h Grey Feldspar Porphyry: white feldspar phenocryst* set in a grey
matrix 9i Pink Feldspar Porphyry: pink feldspar phenocryst* vet in a
pink/grey/white matrix 9j Quartz-Feldspar Porphyry. 9k Quartz Porphyry:
Pukaskwa Gneissic Complex: Hornblende-biotrte bearingTonaiite/Granodiorite/Quartz Diorite, may be plagioclase porphyritic
METASEDDsZNTARY ROCKS
arenite: generally ^X mafic, quartz is the main constituent (ie: >SOX), may contain feldspar
Arkosic Wacke6a Feldspar-Quartz—Biotite Gneiss: generally feldspar dominant,
<5OX quartz, -CIS* biotite. Ab Feldspar-Quartz-Biotite-Amphibole Gneiss: generally feldspar
dominant, ^07* quartz, ^57* mafic 8c Feldspar—Quartz-Amphibole Gneiss: generally feldspar dominant,
<5O% quartz. ^535 amphibole
Wacke 5a
5b
5c
Biolite—Feldspar—Quartz Gneiss: generally feldspar dominant,<50% quartz. J-15% biotiteBiotite—Amphibole—Feldspar Quartz Gneiss: generally feldspardominant, <50% quartz, >15% maficAmphibole-Feldspar-Quartz Gneiss: generally feldspar dominant,<50% quartz, 5-1525 amphibole
METAVOLCANIC ROCKS
Felsic Volcanic Rocks: quartz, <5% mafic4a Felsic Fragmental: white feldspar pb.en.os set in aphanitic white
matrix
Intermediate Volcanic Rocks: quartz, 5 to 50/5 mafic 3a Massive Tuff/Flow:3b Crystal Tuff: contains quartz ? feldspar phenocrysta 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quartz-feldspar flattened
Mafic Volcanic Rocks: generally no quartz and approz equal proportions ofmafit* and plagioclase
2a Massive Flow: 2b Pillowed Flow:2c Feldspar—Amphibolite: ^OX amphibole, feldspar 2d Quartz-Amphibolite: >7Q% amphibole, quartz 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs in white
to greenish white lenses
ROCKS OF UNKNOWN ORIGIN
Q2SS (QSS) Quartz-Seridte SchistQESS (QES) Quartz-eye Sericite SchistQEP Quartz-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
d SE TA SI
PR PY
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KF EP Bl
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMPQTZ FQV
END BRX CRN PEG AFC MSV FOL
GarnetAmphiboleQuartzFeldspar—Quartz vein
MACBIOFELD
TEXTURES
BandedBrecciatedCrenula tedPegmatiticAphanitic to fine grainedMassiveFoliated
PPH XEN PPB CGR FRG DET SCH
MagnetiteBiotiteFeldspar
PorphyriticXenolithicPorphyto blasticCoarse grainedFragmentalDetritalSchistose
-Q j
STRUCTURAL SYMBOLS
Small Scale FI Fold Minor Fold Axia F2 M-Fold Axis ra M-Fold Axis F2 S-Fold Axis FS S-Fold Axis F2 W-Fold Axis F3 W-Fold Axis F2 Z-Fold Axis P3 Z- Fold Ana
BeddingBreccia Clasts
S3 FoliationS3 FoliationSI /SO Compositional Banding
D3 FractureQT fr
QjT E
OTHER SYMBOLS
OUTCBOP LOCATION WITH KOCKTYPE
3 CLAIMPOST
'2 DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RCVER OR LAKE SHORE
GEOLOGICAL CONTACT
UTHOLOGICAL UNIT
ROAD
TRAIL
FOLD AXES
FAULT
^"- CUFF
-284E GSSD "N8 LABEL
"j GRID STATION (100m interval)
" f BASE OF SLOPE (may be swamp boundary)
BEAVER DAM
2
89
6
KEY TO MAP SHEETS
DPLACER DOME C/^JADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
2. 160GEOLOGY MAP
(SHEET 4)
DATE: April, 1995
SCALE: 1 : 2500
ORIG BY: G S DRAWN BY: CCD
NTS REF:42 C/12
DWG.NO. 9
FILE: WRGL04.DWG G \WR(VER\ACAOCWGS\^EDIS4\ REPORT
270 ——
PondGILES
BAY
GO/GAR
3C/FRGRIVERWHITE •i—.5 (minor 6)
3C/FRG
HEMLO FAULT
PICKEREL
BAY
LEGEND
INTRUSIVE ROCKS
Late Maflo Dike (Diabase): appro* equal proportions of plagioclase and pyroxene
Early Mafic Dike. Sill: foliated, deformed gabbro, amphibolite or biotite amphibolite
Felsic to Intermediate Intrusive Rocks9a Granite: <6X maflo, ^X quarts, may be porphyriticOb Granodiorita/Diorita: >6X mafic, ^X quarts9d Syenite: ^X mafic, ^K quarts9e Pegmatite Dike: coarse to very coarse grained feldspar ± quart* ±
mica9f Aplite Dike: quarts le feldspar, no maflos 9g Felsic Dike: 9h Grey Feldspar Porphyry: white feldspar phenocryst* set in a grey
matrix 91 Pink Feldspar Porphyry: pink feldspar phenocryst set in a
pink/grey/wbite matrix 9J Quarts-Feldspar Porphyry: 9k Quarts Porphyry:
Pukaskwa Gneissic Complex: Hornblende-biotite bearingTonalite/Granodiorite/Quarts Diorite, may be plagioclase porphyritic
METASEDIMENTARY ROCKS
Arenite: generally ^X mafic, quarts it the main constituent (la: ), may contain feldspar
Arkosic Wacke6a Feldspar-Quarts~Blotlte Gneiss: generally feldspar dominant,
^OX quarts, *:16X biotite, 6b Feldspar-Quarta-Biotite-Amphibole Gneiss: generally feldspar
dominant. <60% quartz. <1B% mafic 60 FeUspar-tuarta-AmpMtQl
c60X quarts, <1B% amphibole
Waoke6a Biotite-Feldapar-Quarts Gneisst generally feldspar dominant,
^OX quarts, M6X biotite 6b Biotite-Ampbibole-Feldapar Quarts Gneiss: generally feldspar
dominant, ^OX quarts, MBX maflo6c Ampbibole-Feldapar-Quarts Gneiaa: generally feldspar dominant,
quarts, > ^6% amphibole
ItKTAVOLCANIC ROCKS
Felsic Volcanic Rooks: quarts, ^X maflo4a Felsic Fragmental: white feldspar pbenos let in aphanitic white
matrix
Intermediate Volcanic Rocks: quarts, 5 to 50X mafic 3a Massive Tuff/Plow:3b Crystal Tuff: contains quarts t feldspar phenocryst* 3c Lapilli Tuff: monolithic or heterolithic lansea, commonly consists of
quarts-feldspar flattened
Mafic Volcanic Rooks: generally no quarts and approx equal proportions ofmafic and plagioclase
2a Massive Flow: 2b Pillowed Flow: 2o Feldapar-Ampblbolite: >70X amphibole, feldspar
Quarts-Ampbibollte: >70X amphibole, quartsPoker Chip Plagioclase Amphibolite: plagioclase occurs in whiteto greenish white lenaea
2d 2e
ROCKS OF UNKNOWN ORIGINQZSS (Q88) Quarts-Serloite SchistQBS8 (QES) Quarts-eye Sericite SchistQEP Quarts-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
CLSE TA SI
PRpy
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KF EP BI
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMPQTZ FQV
BND BRX CRN
GarnetAmphiboleQuartzFeldspar-Quarts vein
AFG MSV FOL
TEXTURES
Aphanitic to fine grainedMassiveFoliated
BandedBrecciatedCrenulated
MAG MagnetiteBIO BioliteFELD Feldspar
PPHXEN
FRGDET SCH
FragmentalDetritalSchistose
STRUCTURAL SYMBOLSSmall Scale FI Fold Minor Fold Axis FZ M-Fold Axis FS M-Fold Axis W S-Fold Axis F3 S-Fold Axis F8 W-Fold Axis F3 W-Fold Axis F2 Z-Fold Axis F3 Z-Fold Axis
BeddingBreccia Clasts88 FoliationS3 Foliation81/80 Compositional BandingD3 Fracture
^ g
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
Q CLAIMPOST
(•) DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
GEOLOGICAL CONTACT
LITHOLOGICAL UNIT
ROAD
TRAIL
FOLD AXIS
FAULT
CLIFF
L284E
"j GRID STATION (100m interval)
BASK OF UIUVK (may be swamp boundary)
XXX X X BEAVER DAM
IS
1
8
^Ymg
6
KEY TO MAP SHEETS
D PLACER DOME CANADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP(SHEET 5)
DATE: April, 1995
SCALE: 1 :2500
ORIG BY: GS DRAWN BY: CCD
NTS REE: 42 C/12
DWG.NO. 10
EI LE: WRGL05.DWG G:\WRIVER\ACADDWGS\GEOL94\REPORT
280
GILES
^^ Humin K
- "3/PXEAST GRID SHOWING
(WEST TRENCH)
EAST GRID SHOWING
(EAST TRENCH)
HEMLO FAULT
l
LEGEND
INTRUSIVE BOCKS
Late llaHo Dike (Diabase); appro* equal proportion* of plagioclase and pyroxene
Early Mafic Dike, Sill: foliated, deformed gabbro, amphibolite or biotite amphibolite
Felite to Intermediate Intrusive HookaOa Granite: ^X mafic, XiX quarts, may be porphyriticOb Granodiorlte/Diorite: ^H mafic, ^X quarts9d Syenite: C6X mafic. <6X quart*Qe Pegmatite Dike: coarse to very ooarae (rained feldspar ± quarts ±
micaBf Aplite Dike: quarta tt feldspar, no mafic* B( Felsic Dike: Bh Grey Feldspar Porphyry: white feldspar phenocryst* set in a grey
matrix 01 Pink Feldspar Porphyry: pink feldspar phenocryst* set in a
pink/grey/wbite matrix 9J Quarts-Feldspar Porphyry: fik Quart* Porphyry:
Pukaskwa Gneissic Complex: Hornblende-bloUte bearingTonalite/Granodiorite/Quarts Diorite, may be plagioclase porphyritic
METASEDIMENTARY ROCKS
Arenite: generally ^5S mafic, quarti la the main constituent (le: ^OX). may contain feldspar
Arkosic WackeAa Feldapar-Quarta-Biotite Gnei**: generally feldspar dominant,
^0* quartz, UfiX biotite, 6b Feldspar-Quartz-Biotite-Amphlbole GneiM: generally feldspar
dominant, ^QX quarts, < ltit malic .^ . 6c Feldspar-Quarta-Ampblbole Qnvlajn fTOtrally faldapar dominant,
^ox quart*, <^6X ampblbol*Wacke
6a BloUte-Feldspsr-QuerU Gneiss: generally feldspar dominant,^0* quarts, >16X biotite
Bb Biotite-Amphibole-Feldspar Quarts Gneiss: generally feldspardominant, ^OX quarts, MBX mafic
So Ampbibole-Feldspar-Quarts Gneiss: generally feldspar dominant, quarts, M6X amphibole
METAVOLCANIC ROCKS
Feliio Volcanic Rook*: quarts, ^X mafic4a Felsic Fragmental: white feldspar phenoa *at in aphanitic white
matrix
Intermediate Volcanic Rooks: quarts. B to BOX mafic aa Massive Tuff/Flow:3b Crystal Tuff: contains quarts ? feldspar phenocryst* 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quarts-feldspar flattened
Mafic Volcanic Rooks: generally no quarts and approx equal proportions ofmafic and plagioclase
2a Massive Flow: 2b Pillowed Flow:to Feldapar-Amphlbolite: ^OX amphibole, feldspar 2d Quarts-Ampbibolite: ^OX amphibole, quarts 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs in white
to greenish white lenaes
ROCKS OF UNKNOWN ORIGINQZS8 (QSS) Quart i-Sericite SchistQESS (QES) Quarts-eye Sericite SchistQEP Quarts-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
CL SE TA SI
PB PY
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KFBP BI
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMP QTZ FQV
BND BRX CRN PEG AFG MSV FOL
GarnetAmphiboleQuartsFeldspar-Quarts vein
Banded Brecciated
TEXTURES
Aphanitic to fine grainedMassiveFoliated
MAG MagnetiteBIO BioliteFIELD Feldspar
s9 —FRG FragmentalDET DetritalSCH Sohlstove
^ 22-
STRUCTURAL SYMBOLS
Small Scale Fi Fold Minor Fold Axis F2 M-Fold Axis FS M-Fold Axis F3 8-Fold Axis FS S-Fold Axis F2 W-Fold Axis F3 W-Fold Axis F2 Z-Fold Axis F3 Z-Fold Axis
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
H CLAIMPOST
( ) DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
GEOLOGICAL CONTACT
LITHOLOGICAL UNIT
ROAD
TRAIL
FOLD AXIS
FAULT
CLIFF
L284E GRID UNE LABEL
4 GRID STATION (100m interval)
l j BASE OF SLOPE (may be swamp boundary)
BeddingBreccia Clasts82 FoliationS3 Foliation81/80 Compositional Banding03 Fracture
XXXXX BEAVJB DAM
Jk. 1 5056
i
89
KEY TO MAP SHEETS
D PLACER DOME CANADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP(SHEET 6)
DATE: April, 1995
SCALE: 1 :2500
ORIG BY: GS DRAWN BY: C CD
NTS REE: 42 C/12
DWG.NO. 1 1
FILE: WRGL06.DWG C.\WRIVER\ACAODWGS\GEOL94\REPORT
290
POND
\ -J!~USf*fS. ^^ StjHtLfF -i**
538950QN
5389000N
s D . C.S
LAKE
?H 5388500N
B EA VE RPOND
5b,GT,MAG THOR LAKEMASSIVE SULPHIDE
SHOWINGSc/BND
5388000N
LEGEND
INTRUSIVE ROCKS
Late Mafic Dike (Diabase): approx equal proportions of plagioclase and
Early Mafic Dike. Silt foliated, deformed gabbro, amphibolite or biotite
Felsic to Intermediate Intrusive RocksBa Granite: ^35 mafic, >5X quartz, may be porphyritic9b Cranodiorite/Diorite: ^11 mafic. >5X quartzBd Syenite: ^Tt mafic. c55C quartzSe Pefmatite Dike: coarse to very coarse grained feldspar ± quartz ±
micaBf Aplite Dike: quartz Ac feldspar, no mafics 9g Felsic Dike: 9h Grey Feldspar Porphyry: irbjte feldspar phenocrysts set in a grey
matrix 9i Pink Feldspar Porphyry: pink feldspar phenocrysts set in a
pink/grey/white matrix 0j Qnartz-Feldspar Porphyry: 9k Quartz Porphyry:
Pukaskwa Gneissic Complex: Hornblende— biotite bearingTonalite/Granodiorite/Qnartz Diorite, may be plagioclase porphyritic
METASEDIMENTARY ROCKS
Arenite: generally ^X mafic, quartz is the main constituent (ie: ^OX), may contain feldspar
Arkosic Wacke6a Feldspar-Quartz-Biotite Gneiss: generally feldspar dominant,
<50% quart*. ^5X biotite. 6*b Feldspar-Quarti-Biotite-Amphibole Gneiss: generally feldspar
dominant, ^OX quartz, < l5% mafic 6c Feldspar-Quartz-Amphibole Gneiss: generally feldspar dominant,
<50% quartz. •clSSC amphibole
Wacke 5a
9b
Se
Biotite—Feldspar—Quartz Gneiss: generally feldspar dominant, <5OX quartz. >15% biotiteBiotite-Amphibole—Feldspar Quartz Gneias: generally feldspar dominant. <5O% quartz, > ^5^l maficAmphibole—Feldspar-Quartz Gneiss: generally feldspar dominant,
quartz. M5X amphibole
METAVOLCAN1C ROCKS
Felsic Volcanic Rocks: quartz. ^X mafic4a Felsic Fragmental: white feldspar phenos set in aphanitic white
matrix
Intermediate Volcanic Bocks: quartz, 5 to 50X mafic 3a Massive Tuff /Flow:3b Crystal Tuff: contains quartz ? feldspar phenocrysts 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quartz— feldspar flattened
Mafic Volcanic Rocks: generally no quartz and approx equal proportions ofmttftf* and plagioclase
2a Massive Flow: 2b Pfllowed Flow:2c Feldspar— Amphibolite: >70% amphibole, feldspar 2d Quartz-Amphibolite: ^055 amphibole, quartz 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs in white
to greenish white lenses
ROCKS OF UNKNOWN ORIGIN
QZSS (QSS) Quartx-Serictte SchistQESS (QES) Quartz-eye Sericite SchistQEP Quartz-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
d.SE TA St
PR PY
ChloriteSeriateTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KFEP ffi
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMP QTZ FQV
END BEX CBN PEG AFG ItSV FOL
GarnetAmphiboleQuartzFeldspar-Quartz vein
MAGBIOFELD
JTEATUKlSi
BandedBrecciatedCrenulatedPegmatiticAphanitic to fine grainedMassiveFoliated
PPH XEN PPB CGB FRG DET SCB
MagnetiteBiotiteFeldspar
PorphyriticXenolithicPorphytoblasticCoarse grainedFragmentalDetritalSchistose
STRUCTURAL SYMBOLS
Small Scale FI Fold Minor Fold Axis F2 M-Fold Axis FS M-Fold Axis F2 S-Fold Axis F3 S-Fold Axis F2 W- Fold Axis FS W- Fold Axis F2 Z-Fold Axis FS Z-Fold Axis
-Q fr
3P fr
( W, •QTfr
QQT t
Bedding Breccia Clasta52 Foliation53 FoliationS l/SO Compositional Banding
D3 Fracture
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
CLAIMPOST
~ DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
•j*. SWAMP
-—— SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
.——— GEOLOGICAL CONTACT
LTTHOLOGICAL UNIT
r ^ ROAD
, TRAIL
FOLD AXIS
FAULT
CLIFF
L284E
j GRID STATION (100m interval)
- BASE OF SLOPE (may be swamp boundary)
v BEAVER DAM
l
89
6
KEY TO MAP SHEETS
300
DPLACER DOME CANADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY(SHEET 7)
DATE: April, 1995
SCALE: 1 : 2500
ORIG BY: G S DRAWN BY: C CD
NTS REF:42 C/12
DWG.NO. 12
FILE: WRGL07.DWG G.\WR(VER\ACADOWGS\Gf:OlS4\ REPORT
B EA VE R
DC,DO,C
s D .C. \ LAKE
^ . ) ' 'SJ '..iBND *,4 ' - "-
5388500N
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5388000N
5387500N
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DUCK LAKE
LEGEND
INTRUSIVE ROCKS
Late Mafic Dike (Diabase): approx equal proportion* of plagioclase and pyroxene
Early Mafic Dike, Sill: foliated, deformed gabbro, amphibolite or biotite amphibolite
Felsic to Intermediate Intrusive RockiQa Granite: ^X mafic, ^X quarts, may be porphyritioBb Granodlorite/Dioiite: XSX mafic, >SX quart*Od Syenite: ^X mafic, <5X quartzBe Pegmatite Dike: coarse to very coarse grained feldspar ± quartz i
micaBf Aplite Dike: quarts ft feldspar, no mafic* Bg Felsic Dike: Oh Crey Feldspar Porphyry: white feldspar phenocryst* set in a grey
matrix Bi Pink Feldspar Porphyry: pink feldspar phenocryst* set in a
pink/grey/white matrix Bj Quarts-Feldspar Porphyry: fik Quarts Porphyry:
Pukaskwa Gneissic Complex: Hornblende-blotite bearingTonallte/Granodiorite/Quarts Diorite, may be plagioclase porphyritic
METASED1MENTARY ROCKS
Arenite: generally ^X mafic, quartc l* the main constituent (le: ), may contain feldspar
Arkosic Wacke6a Feldspar-Quarts-Blotlte Gneiss: generally feldspar dominant,
quartz, *cl6X biotite,Bb Feldapar-quarU-BiotHe-Amphibole QpetSS: generally feldspar.
60 Feldspar-QuarU-Amphibole Gneisa: gsnerally feldspar dominant. <60X quarts, <16X amphibole
WackeKa BioUte-Feldapar-Quarts Gneiss: generally feldspar dominant,
^0* quarts, >16X biotite 6b Biotite-Amphibole-Feldspar Quart* Qnsiss: generally feldspar
dominant, <60X quarts, >1BX mafic6c Amphibole-Feldspar-Quarts Gneiss: generally feldspar dominant,
quarts, >lfiX amphibole
METAVOLCANIC ROCKS
Felsic Volcanic Rooks: quarts, ^X mafic4a Felsic Fragmental: white feldspar phenoa set in aphanitic white
matrix
Intermediate Volcanic Rooks: quarts, B to BOX mafic 3a Massive Tuff/How:3b Crystal Tuff: contains quarts ? feldspar phenocryst* 3c Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quarts-feldspar flattened
Mafic Volcanic Rooks: generally no quarts and approx equal proportions ofmafic and plagioclase
2a Massive Flow: 2b Pillowed Flow: 2c Feldspar-Amphlbolite! >70X amphibole, feldspar
Quarts-Ampbibolite: >70X amphibole, quartsPoker Chip Plagioclase Amphibolite: plagioclase occurs in whiteto greenish white lenses
2d 2e
ROCKS OF UNKNOWN ORIGINQZSS (QSS) Quarts-Seridte SchistQES8 (QES) Quarts-eye Sericite SchistQBP Quarts-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATIONCL SE TA SI
PR PY
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
GAR AMP QTZ FQV
BND BRX CRN PEG AFG MSV FOL
KV KF EP BI
MINERALIZATION
SL
QUALIFYING MATERIALS
Garnet MAG Amphibole BIO Quarts FELD Feldspar-Quarts vein
TEXTURESBanded PPHBrecciated XBNCranulaUd PPBPegmatitic CGRAphanitic to fine grained FRGMassive DETFoliated SCH
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
agne Biolite Feldspar
Porphytoblaatio Coarse grained Fragmental Detrital Schistose
STRUCTURAL SYMBOLSSmall Scale FI Fold Minor Fold Axis FS M-Fold Axis FS M-Fold Axia F2 8-Fold Axis FS 8-Fold Axis
(X E F2 W-Fold Axia F3 W-Fold Axis F8 Z-Fold Axis F3 Z-Fold Axia
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
CLAMPOST
0 DIAMOND DRILLHOLE LOCATION (LAC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
GEOLOGICAL CONTACT
LITHOLOGICAL UNIT
ROAD
TRAIL
FOLD AXIS
FAULT
CUFF
BeddingBreccia Clasts82 FoliationS3 Foliation81/80 Compositional BandingD3 Fracture
L284E
"j GRID STATION (100m Interval)
BASK O*1 SLOPS (nay b* ewaat? beuadaf?)
XXX X X BEAVER DAM
1 2 3
7^ ^ x^x x(* xx1
x
4
P̂5
9
6
KEY TO MAP SHEETS
I
D PLACER DOME C/^NADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP(SHEET 8)
DATE: April, 1995
SCALE: 1 :2500
ORIG BY: GS DRAWN BY: CCD
NTS REF:42 C/12
DWG.NO. 13
FILE: WRGL08.DWG G.\WRIVER\AODDWGS\GEOL94\ REPORT
310
Beaver Pond
Qd/PPH ^ 9d7PPH
2a (minor 2c)
S i r|,,,.,i,
n\ ™t~™r^^^,i"s-V \ WeqA/'MIJ, J 4*
-
f "qr1 '!'" .
- v \ 6 -"H,indr,l Alll|, \l H.I DI \ V I'll) Am| 01. Mrl.ivi-M-l.i "l /' \ l Irtlhl. ,l
GOVDALAKE6 c "r" V-
^^S ^^ Mi iv j MV \ v
2
: v'"-. TRM UV V \
f ) Art Dyke \ ^V ' Cr.ii MV \
LEGEND
INTRUSIVE ROCKS
Late Mafic Dike (Diabase): approz equal proportions of plagioclase and pyroxene
Early Mafic Dike, Sill: foliated, deformed gabbro, amphibolite or biotite amphibolite
Felsic to Intermediate Intrusive RocksOa Granite: ^35 mafic, ^X quarts, may be porphyriticQb Granodiorite/Diorite: ^X mafic, ^X quartzOd Syenite: ^X mafic, c5X quarts9e Pegmatite Dike: coarse to very coarse grained feldspar i quart* ±
mica9f Aplite Dike: quarts tt feldspar, no mafics 9g Felsic Dike: Oh Grey Feldspar Porphyry: white feldspar phenoorysts set in a grey
matrix 01 Pink Feldspar Porphyry: pink feldspar phsnocrysts set in a
pink/grey/white matrix Oj Quarts-Feldspar Porphyry: Ok Quarts Porphyry:
Pukaskwa Gneissic Complex: Hornblende-blotite bearingTonalite/Granodiorita/Quarts Diorite, may be plagioclase porphyritic
META8BDIMENTARY ROCKS
Arenite: generally ^X mafic, quarts is the main constituent (le: ), may contain feldspar
Arkosic Wacke6a Feldspar-Quarts-Biotite Gneiss: generally feldspar dominant,
^QX quarts, ^5X biotite, Bb Feldcpar-Quarts-Biotite-Amphibole Gneiss: generally feldspar
dominant, <50% quartz, •clSX mafic
^OX quarts, amphibole
Waoke6a Biotite-Feldspar-Quarts Gneiss: generally feldspar dominant.
^OX quarts, M6X biotite 6b BioUte-Amphlbole-Feldapar Quarts Gneiss: generally feldspar
dominant, ^OX quarts, :*1SX mafic60 Ampbibole-Feldspar-Quarts Gneiss: generally feldspar dominant,
quarts, >^6X amphibole
METAVOLCANIC ROCKS
Felsic Volcanic Rooks: quarts, ^X mafic4a Felsic FragmenUl: white feldspar phenos set in aphanitic white
matrix
irmediate Volcanic Rooks: quarts, B to 60X mafic 3a Massive Tuff/Flow:3b Crystal Tuff: contains quarts ? feldspar phenoorysts 3o Lapilli Tuff: monolithic or heterolithic lenses, commonly consists of
quarts-feldspar flattened
Mafic Volcanic Rooks: generally no quarts and approx equal proportions ofmafic and plagioclase
2* Massive Flow: 2b Pillowed Flow:2c Feldspar-Ampbibolite: ^OX amphibole, feldspar 2d Quarts-Amphibolita: ^OX amphibole, quarts 2e Poker Chip Plagioclase Amphibolite: plagioclase occurs in white
to greenish white lenses
ROCKS OF UNKNOWN ORIGINQZSS (QSS) Quarts-Serloite SchistQESS (QBS) Quarts-eye Sericite SchistQEP Quarts-eye PorphyryQR Weakly Sericitic Felsic Volcanic
ALTERATION
CL 8E TA SI
PR PY
ChloriteSericiteTalcSilica (pervasive)
Pyrrhotite Pyrite
KV KFIP BI
MINERALIZATION
SL
K-feldspar (veins) K-feldspar (pervasive) Epidote Brown Biotite
Sphalerite
QUALIFYING MATERIALS
GAR AMP QTZ FQV
BND BRX CRNmMSVFOL
GarnetAmphiboleQuartsFeldspar-Quarts vein
TEXTURES
BandedBrecciatedCrenulatedEMnntJMt*Aphanitic to fine grainedMassiveFoliated
MAG MagnetiteBIO BioliteFELD Feldspar
PPH XENPPB COB FRG DET SCH
PorphyriticXenolilhlcPorphytoblasticCoarse framedFragmentalDetritalSchistose
STRUCTURAL SYMBOLS
Small Scale FI Fold Minor Fold Axis F2 M-Fold Axis F3 M-Fold Axis F2 S-Fold Axis FS 3-Fold Axis F2 W-Fold Axis F3 W-Fold Axis F2 Z-Fold Axis F3 Z-Fold Axis
J) j •JJ) j
BeddingBreooia Clasts82 FoliationS3 FoliationSI/80 Compositional BandingD3 Fracture
4 gg
OTHER SYMBOLS
OUTCROP LOCATION WITH ROCKTYPE
CLAIMPOST
0 DIAMOND DRILLHOLE LOCATION (UC MINERALS)
SWAMP
SWAMP BOUNDARY
SMALL OUTCROP LOCATION
RIVER OR LAKE SHORE
GEOLOGICAL CONTACT
LITHOLOGICAL UNIT6JROAD
TRAIL
FOLD AXIS
FAULT
CLIFF
L284E GRn) UNE
4 GRID STATION (100m interval)
J" J BASE OF SLOPE (may be swamp boundary)
XXXXX BEAVER DAM
1
Q t .6
KEY TO MAP SHEETS
O
D PLACER DOME CANADA LIMITED.PROJECT NO. 505 WHITE RIVER PROPERTY
GEOLOGY MAP(SHEET 9)
DATE: April, 1995
SCALE: 1 :2500
ORIG BY: GS DRAWN BY: CCD
NTS REF:42 C/ 12
DWG.NO. 1 4
FILE: WRGL09.DWG G.\WRIVER\ACADDWGS\GEOL04\REPORT
320
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