ID,#,Part Number,Capsule Geology
036CSE0006,1,1,"The Ray Showing is a small uranium showing exposed in Aphebian gneiss and pegmatite over 29 meters at surface. Work included airborne scintillometer, mapping and ground investigation of anomalies in 1975-76. In 1978 a ground radiometric survey and diamond drilling were completed. Indicated resources are listed as 75,000 at 1.00 lbs/t U3O8 to a depth of 60 m (1978). This showing is small and did not continue at depth."
037CNE0010,2,1,9 significant showings.
055ENW0007,3,1,"Turquetil Lake Northwest is a gold showing associated with carbonate (-quartz) alteration within sheared mafic to intermediate volcanics .  The host volcanic are part of the Archean Kaminak Group supracrustral rocks in the Churchill-Hearne Structural Province.  The alteration zone (shearing) is traceable in 4 seperate directions (north, northwest, southwest and southeast) for up to 12 kilometres.  Gold mineralization has been encountered in drill core on the eastern side of the  river in two carboante altered, sheet-like zones which strike northeast and dip steeply northwest (varying to north-northeast).  Gold mineralization in these altered zones was encountered over a strike lenght of 940 metres.  On the western side of the Turquetil River a single gold-bearing, carbonate altered (shear) zone occurs.  This zone is traceable for about 1200 metres and is situated on the hanging wall side of a northeast trending fault thats dips northward.   These zones have alteration widths of up to 100 metres (DIAND, Exploration Overview 1988; reference 1988).  Drill hole results include 13.1 metres grading 7.27 grams/tonne gold and 8.5 metres grading 9.21 grams/tonne gold.  A resource estimate was preformed on the Turquetil Lake property with a probable resevre figure of 3,800,000 tonnes grading 2.4 grams/ton which includes a drill-indicated reserve of 550,000  tonnes grading 6.31 grams/tonne gold.  The zone is still open along strike and at depth.  A brief history of the area starts with exploration work in the Turquetil Lake area by Giant Yellowknife Mines in the 1960's followed by geological mapping completed in the 1970's by the Geological Survey of Canada.  Essex Minerals Company, in 1976, intersected a gold-bearing zone assaying 0.212 oz/ton over 43 feet during a drilling program.  Follow-up ground geophysicals was preformed in the late 1970's, along with additional diamond drilling.  Nobal Peak Resources and Dejour Mines Limited, staked claims over the mineralized"
055ENW0007,4,2,"areas around Turquetil Lake.  Regional and detailed mapping, diamond drilling, rock sampling (including channel sampling) and airborne geophysics were used to better define the gold-bearing structures since 1988."
055JNW0001,5,1,"The gold-bearing iron fromation comprising the Discovery prospect occurs within the Archean Kaminak Group supracrustal rocks.  The iron formation is along the Pyke Fault which extends for 50 kilometres (3 to 5 kilometres wide) through the Meliadine property.  Three structurally distinct  folds along the same iron formation makes up Discovery which has a strike lenght of 250 metres and a depth of 466 metres.  In 1989 the showing was first discovered through sampling and geophysical means.  Since then tens of drill holes and airborne geophysical surveys were used to better define the showing.  The diamond drilling has yielded gold values of 19.89 grams/tonne  over 4.7 metres.  The showing is reported to contain 1,386,000 tonnes of 6.8  grams/tonne gold (proven) and a probable resource of 455,000 tonnes grading 6.47 grams/tonne gold."
055KNE0144,6,1,"The F-Zone is an cherty iron formation (magnetite-poor) with gold-bearing quartz veins.  Theses quartz veins occur in the high strained (fold hinges) areas of the structure.  A 4,300 foot strike lenght is reported for the zone which is one of several iron formations comprising the Wes Meg prospect.   Sulphide mineralization in the iron formation includes mainly arsenopyrite and [pyrite with lesser chalcopyrite.    Since at least 1994,  tens of drill holes have been completed on the zone and an indentified resource has been calculated based ion surface drilling results.  The indicated reserve for the F-Zone are 1,800,000 tonnes grading 7.8 grams/tonne gold giving 0.4 million ounces of gold (reference 19980629Comaple)."
055KSW0041,7,1,"The area is underlain by the easterly part of the Rankin - Ennadai Greenstone Belt.  This belt, which is up to 380 km long, is comprised of three east-northeast trending basins containing both Archean and Aphebian rocks.  Archean rocks of the Kaminak Supergroup (Lewry, Sibbald and Schledewitz, 1985) are comprised of volcanic sequences, sediments and minor iron formation units.  At least four complete mafic-felsic volcanic cycles are recognized (Ridler and Shilts, 1974).   Recent mapping in the Tavani map area has lead to further subdivision of the Kaminak Supergroup into the Kasigialik Group and the Tagiulik Formation (Park and Ralser, 1990).  The Kasigialik Group encompasses a volcanic-sedimentary sequence comprised of mafic pillow lavas (Atungag Formation), mafic and felsic volcanics, volcaniclastics, breccias and conglomerates (Akliqnaktuk Formation) and quartzofeldspathic turbidites (Evitaruktuk Formation).  The Taguilik Formation is dominantly quartz poor turbidites with banded ironstones.  Archean rocks in the area generally trend northeast-southwest.   Kaminak Supergroup rocks are unconformably overlain by Aphebian age sediments of the Hurwitz Group which  form two elongate northeasterly striking domains offset slightly by northwest trending dextral faults.  In this area, Hurwitz Group is comprised of two main ""facies associations"" - orthoquartzite (Kinga Formation) and lithic arkoses (Tavani Formation).    Archean and Aphebian age intrusions, mafic to felsic in composition, occur throughout the area.   At least three phases of regional deformation are recognized in the Tavani area, as well as a localized Archean d?collement zone at the base of the Taguilik Formation (Park and Ralser, 1990).  Arch"
055KSW0041,8,2,"ean D1 corresponds to large scale F1 folds, pervasive S1 foliation and bedding parallel high strain zones.  D2, also Archean, is characterized by northeast trending open to tight folds and steeply dipping shear zones.  Proterozoic deformation, during the Hudsonian Orogeny, resulted in the folding of both the Hurwitz Group and the Kaminak Supergroup rocks.                    Age dating indicates granite emplacement as syn-D1 and post-D2 (2659 +/- 4.6 Ma).  Metamorphism in Archean rocks varies from sub-greenschist to upper-amphibolite near intrusive bodies, while Hurwitz Group reach sub-greenschist facies.  A migmatite occurs in the western part of the map area and is thought to have been thrust emplaced from the west (Park and Ralser, 1990).                    Detailed mapping by Al Miller of the GSC (Miller, 1989) divided the predominantly mafic volcanic sequence into three meta-volcanic units with minor meta-sedimentary units.  The entire sequence trends northeast-southwest, dips northwest at 40? to 60? and is interpreted to be an upright homocline.  The three volcanic units (V1-V3) are basically comprised of pillowed and massive flows while the sedimentary units may contain tuffaceous sediments, pyritic chert and black slates.  Park and Rasler (1990) mapped these rocks as belonging to the Akliqnaktuk Formation of the Kaminak Supergroup.                    The Fat Lake showing occurs in one of two quartz diorite (termed the 'Fat Lake' suite by Park and Ralser, 1990) sills characterized by 5 mm to 10 cm sized feldspar crystals in a medium grained, equigranular matrix.  The Fat Lake intrusion occurs at/near the contact of the V1 volcanic unit and the S1 sedimentary unit (Miller, 1989).  Contacts of the Fat Lake sill are sheared while those of the Caribou Horn intrusion,"
055KSW0041,9,3,"further northeast, are not deformed.  The shears trend about 050?, with related shears at 030?, and imply dextral movement.  The shears are believed to be important to both gold mineralization and in influencing the deposition of Proterozoic Hurwitz Group sediments (Miller, 1989).                    Gold mineralization is found in quartz veins in supplemental shears which may be up to 5 m wide and 300 m long (Skillings, 1986; AR 081936).  Veins are preferential to the quartz diorite sill and appear to die out within meters of the contact with the surrounding mafic volcanic rocks.  The quartz veins are generally 0.3 m wide and from 25 to 100 m long (AR 081936) and highly irregular (may be folded or boudinaged) demonstrating several opening/filling phases (Miller, 1989).  Between two and four generations of quartz are recognized  (Skillings, 1985; Skillings, 1986).  Veins contain varying amounts of carbonate, chlorite and disseminated pyrite, chalcopyrite, sphalerite, galena and visible gold.  There are reportedly numerous quartz veins in the area but four (#99 - #103) veins have received the most interest.                    Alteration in the quartz diorite consists of black chlorite associated with the quartz veins and epidote-like discoloration of the intrusive between the veins (Miller, 1989).  The shear zones are generally chloritized and carbonitized.  Some alteration of the magnetite and titanite is also noted in the sill.                    Gold mineralization is dated as being Archean.  Park and Ralser (1990) state that the auriferous veins are ""demonstrably pre-D2 on structural criteria and therefore Archean"" and model lead dates from galena in the veins returned dates of 2652 Ma (Abitibi lead model) and 2694.5 Ma (Western Superior lead model)."
055KSW0041,10,4,"  Work on this showing reportedly occurred as far back as the 1940s when Hudson Bay Mining and Smelting blasted trenches (AR 080406).  In the 1970s the property was covered by the IT claims and grab and channel samples were collected from quartz veins and carbonate shear zones by a Coniagas/Denison/J.A. Syme joint venture group.  The best value from their sampling was 2.85 opt Au and 0.61 opt Ag over 1 foot.  At $100 per ounce price of gold, it was recommended no further work be done as the gold in the veins was high grade but not sufficient in size (AR 080406).  Borealis Exploration Limited first examined the ground as part of the exploration program on prospecting permit 1070 (just north of Fat Lake).  The showing was then staked as the SUSAN claims and Borealis also obtained numerous other prospecting permits in the 55K/4 map sheet to protect ground for further gold exploration.  Borealis work history on this particular showing and others in the area is somewhat confusing and hard to decipher from the various reports and the following is a brief summary, as best as can be determined for the Fat Lake deposit.  In  1985, Borealis did detailed mapping and grab, channel and pan sampling on the A grid or South Zone (not to be confused with the South Gossan zone) of Fat Lake.  (The North Zone or B grid actually refers to the North Occurrence (see NT MINFILE showing 055KSW0042).).  The best value came from sample 15 which contained 4.02 opt Au (grab).  They also did Max-min suveys but did not get any anomalies however a magnetic survey delineated a response coincident with a northeast-southwest trending shear zone.  Exploration work in 1986 consisted of more detailed mapping, sampling, geophysical surveys and"
055KSW0041,11,5," diamond drilling.  They did EM and magnetic surveys and outlined an EM conductor under Fat Lake which was consequently drilled with 6 holes (593 m).  The holes intersected iron formation and shear zones but no good gold values were returned from sampling (AR 082788).  Detailed mapping, trenching (not alot of details about this) and channel sampling were also completed.  The best sample returned a 6.8 gpt Au value but the width of the channel is not known.  Forty-five holes were  then drilled on the Fat Lake showing totalling 1586 m. The following year, 8 more drill holes were completed on the Fat Lake site and with encouraging results they decided to do some underground development.  Borealis drove a 70 m decline shaft to the -17 m and drifted about 75 m along the length of one of the four main veins (Vein 101) for underground mapping and sampling.  Later that season, another 25 drill holes were completed (1270 m ) with a best result of 14.3 opt Au over 1.10 m from a vein named Sofyas Vein (not sure if this is one of the original four veins numbered 99-103).  A test mill also opertated for three days processing 150 tonnes of ore from Vein 101 (AR 082788).  In 1988, a 3 m by 3.5 m ramp was driven to the 960 (-40 m) level (AR 082788, 1988 Annual Report) and 56 samples were collected from the walls of the ramp.  In addition, 8 drill holes were completed for 1271 m.  Ore reserves were calculated based on 72 inclined holes drilled on the #99-103 veins (of which only 36 had acid dip tests) and reserves were only calculated for the four main veins.  They calculated reserves of 13,895 tonnes at 15.03 grams/tonne Au (AR 082788, page 14).  In the same year, the 1988 Annual Report for Borealis Exploration Limited (released March 31, 1988) sta"
055LSE0056,12,1,"Gold mineralization within the Cache Zone is associated with pyrite, quartz veining, structural features and alteration typical of major producing gold deposits (Troupe et al., 1989).  The deposit occurs in a conformable shear zone within an altered felsic to intermediate volcanogenic unit adjacent to a contact with mafic volcanic flows.  Diamond drilling established that gold mineralization extends more than 200 m vertically, the width and grade increasing with depth.  The gold is associated with disseminated, euhedral pyrite.  Five parallel but distinct zones of mineralization have been recognised.  Channel samples taken by Noble Peak (1989) across a 1 m wide quartz vein gave average assay values of 1.71 oz/ton gold over 4 metres.  The discovery channel sample assayed 58.6 g/t gold across 4 m of quartz stockwork.  A possible reserve of 364 000 tonnes grading 9.26 g/t gold was indicated by the 1988 drilling program.  Four holes were drilled in 1989 in order to outline the extension of the Cache zone 100 m below the 1988 holes.  It is now thought that the mineralized zone plunges to the west, has a strike length of 250 m and a depth of 300 m (EMPR-GNWT, 1995).  Five grab samples were taken by D.A. Irwin (1995) just 300 m south-southeast of the main showing of the Cache Zone.  Assays show anomalous gold for four of the five samples, with values ranging from 840 - 7560 ppb gold (Irwin, 1995)."
055MNW0002,13,1,In Dec. 1971 Pan Ocean Oil Ltd. estimated average width to be 6 feet of 0.46% U3O8.
055NSE0001,14,1,"The Tiriruniak Zone is a quartz-rich shear cutting iron formation, basalts and sediments of the  Archean Kaminak Group.  Drill core contains white mineralized quartz veins (possible stockwork) containing ankerite, arsenopyrite and locally pyrrhotite.  The mineralized zone contains significant gold assays which include 0.98 oz/ton gold over 7.7 feet (1998 dirll hole 205).   Local chert-rich  breccia zones were intersected in drill core.  The showing consists of two parallel zones termed the Upper Contact and Lower Shear.  A mineralized trend extending about 1 kilometre was delineated with diamond drilling on the Upper Contact Zone.  A resource calculation of 8,000,000 tonnes grading 11.1 grams/tonne gold (identified reserve) was completed in 1998 (reference 19980629Comaple)."
056DSE0007,15,1,Ground surveys and 12 diamond drill holes totalling 2234 feet cut values in 1970.  Estimated 500 tons of U3O8 and 1000 tons of MoS2.
065HNE0001,16,1,"The Heninga Lake volcanogenic massive sulphide deposits are situated within the Rankin-Ennadai greenstone belt in the Archean Hearne structural province. Mineralization occurs as three discrete lenses in ash tuffs of the Kaminak Group, near the top of Leggetts (1980) Formation A, a sequence of interlayered intermediate and felsic lapillistones, ash tuff, volcaniclastic sediments, crystal tuffs and mafic flows or sills. The overlying Formation B comprises a sequence of intermediate to mafic flows, flow breccia, ash tuff, lapillistone, breccia, volcaniclastic sediments and minor oxide facies iron formation. Layered rocks generally strike eastnortheast and dip vertically or steeply to the south. Archean rocks have been regionally metamorphosed to the greenschist facies except in contact zones around some larger intrusive bodies, where a higher grade is developed. Large scale NNE trending isoclinal folds are the dominant structural influence in the vicinity of the deposits.  Three sulphide lenses occur in Member A4 of Formation A, a 50 - 150 m thick sequence of intermediate to felsic ash tuff and lapillistone with lesser tuffaceous sediments and chert. The Western Zone consists of a single, 3 - 4 m thick and 400 m long lense, while the smaller Eastern and Central lenses are up to 3 m thick and 90 m long. All three lenses thin rapidly laterally, dividing into multiple narrow horizons of semi-massive to massive sulphides interbedded with chert and ash tuffs.  The Central and Western zones both consist of a stratiform, bedded horizon of sphalerite, pyrite and minor galena with a central, relatively structureless core of chalcopyrite, pyrite and minor pyrrhotite."
065HNE0001,17,2,"A discordant stringer sulphide zone within a sericite-quartz-chlorite-carbonate alteration pipe underlies the massive sulphides. The Eastern zone lacks a feeder pipe and is dominantly a horizon of bedded sphalerite, pyrite, galena, chalcopyrite and tetrahedrite.                       Drilling has established a reserve of about 5.5 million tonnes grading 9.0% Zn, 1.3% Cu, 67.0 g/t Ag and 1.0 g/t Au."
065INE0001,18,1,"The Ferguson Lake Cu-Ni sulphide deposit is located in the Archean Hearne Structural Province, part of the previously designated Churchill Province. Mineralization is present as a 20 km long sulphidic zone situated in an east-west trending package of mafic volcanics sandwiched between various high grade ortho and paragneissic terranes. The volcanic rocks have been metamorphosed to upper amphibolite to granulite facies. Several syn to post-tectonic gabbros and late syenite intrusives cut the stratified rocks.  The most abundant rock type in the immediate vicinity of mineralization is a medium grained mafic amphibolite containing 30 - 60% hornblende. No primary textures remain although a moderate to strong subhorizontal lineation is present. Sulphide mineralization occurs in a 50 - 200 m wide, medium to coarse grained hornblendite subunit that has been interpreted as a metamorphosed ultramafic sill within the amphibolites. It contains more than 60% hornblende, plagioclase and minor garnet and locally displays modal banding probably related to metamorphism. A moderate foliation or lineation is often present.  The main sulphide zone generally occurs as a single discrete horizon up to 10 metres thick but may locally comprise a series of narrow parallel horizons. A strong gossan marks the zone in outcrop. Mineralization consists of both ""breccia"" and ""stringer"" sulphides. The former type is found in discontinuous pods up to 50 cm thick consisting of 60 to 90% pyrrhotite. Inclusions of well-formed quartz and hornblende crystals as well as aggregates of both are common in the main part of the zone, which may have led to the brecciated description. In the western part of the sulphide horizon, abundant magnetite is present in the form of semi-rounded clots rimmed by sulphide."
065INE0001,19,2,"Stringer type mineralization is more continous, consisting of stratabound veinlets of chalcopyrite, pyrite and pyrrhotite comprising up to 10% by volume of the hornblendite. Amphibolite immediately adjacent to sulphides is garnetiferous. Canadian Nickel (Inco) carried out a large program of geophysics, mapping, diamond drilling and bulk sampling in the early 1950s, eventually outlining approximately 7.3 million tons grading 0.87% Cu and 0.75% Ni in the main mineralized zone. The deposit was traced over a strike length of 7700 metres and to a depth of about 250 metres. In 1987, Homestake Mineral Development Company optioned the property and sampled it for PGE. Samples of breccia style mineralization contained from 50-700 ppb Pt and up to 5000 ppb Pd. Samples of stringer style sulphides contained from 80-800 ppb Pt and 90-1200 ppb Pd. Sulphides also contain erratically anomalous levels of Co (up to several hundred ppm) and Au (up to a few tens or hundreds of ppb)."
065JNE0005,20,1,"The Yathkyed Lake showing is an unconformity-vein type uranium deposit at the margin of the Helikian Dubawnt Group sediments and hosted in the underlying Archean tuffaceous and exhalative sediments. The deposit is stratabound and is delineated as several thin moderately plunging shoots within the interflow sediments.  Work was done in the showing area from 1975-1982 and included airborne radiometric, magnetic and VLF-EM surveys, ground scintillator, magnetic and EM geophysical surveys, geochemical  sampling, geological mapping and diamond drilling. The drill indicated resources of 387,619 tons at 1.05% U3O8 plus  141,934  inferred  tons at 1.24%. The resources were outlined by diamond drilling in an nearly vertical zone 3,600 feet long to a depth of 750 feet. It is stated that this deposit would be difficult to mine without substantial dilution."
066ASW0002,21,1,"The Lone Gull showing is an unconformity related vein type deposit located near the faulted margin of the Thelon Basin. Mineralization is hosted in multiple lithologies. Archean feldspathic wacke and minor pelite, Archean/Proterozoic W-Mo bearing porphyritic granite and Dubawnt group syenitic dykes. The uranium mineralization is close to the surface, down to 175 m and is amenable to open pit mining.  Work on the showing commenced in1974 with the initial field geochemical and geophysical discovery. This was followed by diamond drilling, a biological study, geological mapping, geophysics, geochemical sampling, a gravity survey and in 1988-89 a feasibility study.   The calculated resource for this showing is listed as 2.99 million metric tonnes at 0.61% U3O8."
066GSE0001,22,1,"Mineralization of the Lost Lake showing is syngenetic but remobilized uraninite dissemination within thinly interbedded arkose-siltstone-mudstone of the upper Aphebian Amer group. The showing is near the Thelon unconformity and this Aphebian mineralization may have been upgraded by processes similar to unconformity related vein type uranium mineralization.  Work on the showing commenced in 1977 with a VLF-EM and IP geophysical survey and geochemical sampling. in 1979 diamond drilling was done and in 1984 geochemistry, and a VLF-EM and magnetic geophysical survey was completed. An inferred resource of 900,000 metric tonnes at 0.104% U3O8 is listed."
066HSE0015,23,1,"The Third Portage Lake deposit lies within the Tehek-Sissons greenstone metasedimentary belt of Archean age, in the Churchill Structural province of the Canadian shield.  The belt is subdivided into two groups and one, the Woodburn Lake group, underlies the area of interest.  It is comprised of a northeast-trending sequence of metavolcanic and metasedimentary rocks (Hauseux, 1989).  This supracrustal package is dominated by fine-grained clastics such as greywacke, argillite and rare pelite, but is characterized by the presence of spinifex-textured komatiites and ultramafic schists, oxide and silicate facies iron formations and associated quartzite units (Hughes and Legault, 1993).  Rocks of the Woodburn Group are intruded by Kenoran-age (late Archean) unfoliated granitic plutons and Early Proterozoic-age Amer Group and Hurwitz Group supracrustal rocks rest unconformably on the granties to the northwest and southeast, respectively (Hughes and Legault, 1993).  Metamorphic grade is generally upper greenschist but locally reaches amphibolite facies.  The regional structure involves a large shear zone and complex folding.  The shear zone is typified by brittle features such as fault gouge, breccia and quartz veins in the north and mylonitic features indicative of more ductile deformation in the south.  The Portage Fault Shear Zone trends roughly north-south and dips moderately to the west.  Four phases of folding have been discerned in the area (Hughes and Legault, 1993).  Two phases have been seen in drill core.  The first is isoclinal with tight folds on the order of 10-20 cm across.  These are folded by a more open, asymmetrical set of folds (Hubacheck and Atkinson, 1993)."
066HSE0015,24,2,"Hughes and Legault (1993) argue that the entire supracrustal sequence has undergone significant isoclinal folding and lies within a regional recumbant fold structure.  The Portage Fault Shear Zone (or Third Portage Lake Fault Zone) post-dates the folding phases and may represent the gold fluid conuit for the known mineralization (Hughes and Legault, 1993).  Significant gold mineralization occurs in two settings.  Pyrrhotite-bearing ductile shear zones in magnetite-chert-grunerite iron formation is the most common type of mineralization.  However, higher grade gold mineralization occurs where pyrite has been introduced, either as direct replacement of previously folded pyrrhotite and magnetite or in association with various quartz vein events.  This high grade gold may be related to fold axes (Hubacheck and Atkinson, 1993).  Some of the highest grade assays are contained in sections having 20-50% grey quartz with pyrite,  Values up to 20.5 g/t over 4.8 metres were returned from 1989 drilling on the Third Portage Lake deposit (Barham and Mudry, 1990).  Work has continued on the Third Portage Lake deposit, which has been estimated to hold a resource of over 710 560 oz of gold within 95 metres from the surface, at an average grade of 6.53 g/tonne (cut).  Recent engineering studies indicat that >90% of the resource will likely be accessible by open pit extraction (Cumberland Resources Annual Report, 1996)."
066HSE0016,25,1,"The Third Portage Lake deposit lies within the Tehek-Sissons greenstone metasedimentary belt of Archean age, in the Churchill Structural province of the Canadian shield.  The belt is subdivided into two groups and one, the Woodburn Lake group, underlies the area of interest.  It is comprised of a northeast-trending sequence of metavolcanic and metasedimentary rocks (Hauseux, 1989).  This supracrustal package is dominated by fine-grained clastics such as greywacke, argillite and rare pelite, but is characterized by the presence of spinifex-textured komatiites and ultramafic schists, oxide and silicate facies iron formations and associated quartzite units (Hughes and Legault, 1993).  Rocks of the Woodburn Group are intruded by Kenoran-age (late Archean) unfoliated granitic plutons and Early Proterozoic-age Amer Group and Hurwitz Group supracrustal rocks rest unconformably on the granties to the northwest and southeast, respectively (Hughes and Legault, 1993).  Metamorphic grade is generally upper greenschist but locally reaches amphibolite facies.  The regional structure involves a large shear zone and complex folding.  The shear zone is typified by brittle features such as fault gouge, breccia and quartz veins in the north and mylonitic features indicative of more ductile deformation in the south.  The Portage Fault Shear Zone trends roughly north-south and dips moderately to the west.  Mineralization at the Third Portage Lake North Extension is represented by a UTEM conductor and mineralized frost heave at the surface.  Drilling confirmed suspected anomalous gold associated with iron formation and shearing."
066HSE0016,26,2,"A sequence of drill core comprising cherty iron formation and quartz/muscovite-schist with pyritic and chloritic quartz veins gave a gold of 9.2 g/tonne over seven metres (Hubacheck and Atkinson, 1993).  The 1996 Annual Report for Cumberland Resources Ltd indicates that the North Portage deposit holds a reserve of 259 185 tonnes gold grading 9.31 g/tonne for a total of 77 606 ounces gold."
066HSE0017,27,1,"The Goose Island prospect is located just one km south of Third Portage Lake deposit, which lies within the Tehek-Sissons greenstone metasedimentary belt of Archean age, in the Churchill Structural province of the Canadian shield.  The belt is subdivided into two groups and one, the Woodburn Lake group, underlies the area of interest.  It is comprised of a northeast-trending sequence of metavolcanic and metasedimentary rocks (Hauseux, 1989).  This supracrustal package is dominated by fine-grained clastics such as greywacke, argillite and rare pelite, but is characterized by the presence of spinifex-textured komatiites and ultramafic schists, oxide and silicate facies iron formations and associated quartzite units (Hughes and Legault, 1993).  Rocks of the Woodburn Group are intruded by Kenoran-age (late Archean) unfoliated granitic plutons and Early Proterozoic-age Amer Group and Hurwitz Group supracrustal rocks rest unconformably on the granties to the northwest and southeast, respectively (Hughes and Legault, 1993).  Metamorphic grade is generally upper greenschist but locally reaches amphibolite facies.  The regional structure involves a large shear zone and complex folding.  The shear zone is typified by brittle features such as fault gouge, breccia and quartz veins in the north and mylonitic features indicative of more ductile deformation in the south.  The Portage Fault Shear Zone trends roughly north-south and dips moderately to the west.  Extensional drilling on Goose Island confirmed the presence of a significant gold bearing horizon located 1 km south of the Third Portage Lake showing.  Initial prospecting and mapping in 1989-90 returned anomalous assays ranging from 1 g/tonne to 16.7 g/tonne hosted in sulphidized iron formation."
066HSE0017,28,2,"Follow-up geophysics in 1989 and 1991 indicate a strong, consistent magnetic anomaly with moderate conductivity.  In addition, the 1991 UTEM and magnetics survey reveal the presence of a steeply dipping conductive zone flanking the western side of the magnetic trend, slightly offshore from the Island.  Four holes were diamond drilled on Goose Island in 1991 and best results were returned from a section having 20 - 50% grey quartz with pyrite and pyrrhotite (482.4 g/t over 1 metre) (Hubacheck and Atkinson, 1993).  The 1996 Annual Report for Cumberland Resources indicates a reserve of 976,834 tonnes grading 11.46 g/tonne gold.  The tonnage was calculated over 37 drill holes on 50 metre line spacing with a 5 g/tonne cut-off over a minimum of 2 metre core length."
068HNE0002,29,1,"The Eclipse lead-zinc prospect is situated about 26 km northeast of the Polaris Pb-Zn mine on Little Cornwallis Island. It is one of a number of Mississippi Valley type Pb-Zn deposits occurring in the Cornwallis Lead Zinc district. In this district, mineralization typically occurs in a paleokarst surface developed at an Early Devonian unconformity within Ordovician to Silurian limestones of the Thumb Mountain Formation. The presence of colloform sphalerite in Devonian conglomerate clasts supports a Devonian age for mineralization.  The main lithologies at the Eclipse deposit are a light grey to brown, sublithographic limestone with abundant shaly partings, contributing to rapid mechanical breakdown, and a buff to brown dolomite with common traces of disseminated marcasite.  At least three separate mineralized zones are located along a 2.5 km, northerly trending axis of deformation marked by alignment of cherty rubble patches as well as coincident geochemical and IP anomalies. The northernmost is the largest and consists of two major zones known as the West and East Breccias. Sulphides in the West Breccia occur mainly as massive open space fillings in a fault breccia with a gangue of white, coarsely crystalline calcite and/or dolomite. Sphalerite is the dominant ore mineral and is generally colloform-textured with alternating lighter and darker bands. Galena is abundant locally as irregular crystalline blebs but is erratically distributed. Both minerals are also found as disseminations adjacent to massive sulphides, as weak replacements of breccia fragments and as narrow, irregular fracture fillings.  The East Breccia is similar but of somewhat lower grade. One area within this zone contains more abundant galena, in places as colloform aggregates or layers up to 1 m thick."
068HNE0002,30,2,"An unusual, coarse grained calcite-dolomite rock described as having white/greenish gray salt and pepper texture was noted in many places in both zones. Disseminated crystals of sphalerite and galena and colloform aggregates of sphalerite are distributed throughout this rock type, which is not correlatable between holes. In contrast to the Polaris deposit, little marcasite or pyrite is present.  Except for slight secondary dolomitization of some breccia fragments, little or no alteration is present. Contacts between mineralization and wall rock are sharp and well-defined. However, up to a third of the sphalerite to the drill-tested depth has weathered to smithsonite.  The Centre and South showings occur in narrow breccia zones paralleling the strike of the enclosing dolomites. Angular fragments up to 8 cm in size are cemented with white calcite and/or dolomite. Sphalerite and galena occur in the matrix. Little additional information is available.  Work done on the showing area from 1960-1972 included sampling, diamond drilling, geological mapping, soil geochemistry, and a gravity survey.  Two zones had resources calculated: The West Breccia zone: 1,000,000 t at 12.43% Zn and 2.18% Pb to 50 feet and the East Breccia zone: 170,000 t at 3.6% Zn, 0.5% Pb plus 265,000 t at 3.45% Zn and 2.19% Pb."
075ASE0001,31,1,"The Nickel King deposit is associated with an Early Proterozoic mafic to ultramafic sill on the order of 60 metres thick. The sill intrudes feldspathic to quartzose paragneisses containing granitoid and pegmatoid segregations. Similar segregations in the sill suggest that it predates granulite facies regional metamorphism. Subsequent tectonism, probably coeval with metamorphism, has deformed the sill into a tight to isoclinal fold, the axis of which trends westerly and plunges westerly at about 14 degrees. The two fold limbs dip to the south at 30 degrees and 50 degrees. Two northerly trending, west-side-down faults offset the limbs of the fold.  The sill is highly heterogeneous and includes norite, gabbro, olivine gabbro and pyroxenite. It is altered in places to a fibrous amphibole, probably actinolite or cummingtonite, along with chlorite and biotite. Sulphides occur as irregularly distributed disseminations to semi-massive segregations in the sill and are not necessarily associated with alteration. Drill information suggests that total sulphide content increases towards the nose of the fold. Sulphide minerals are mainly pyrrhotite and chalcopyrite. Pentlandite, often partly altered to a bravoite series mineral, tends to occur as inclusions, bands and flame-like exsolutions in pyrrhotite.  Cu and Ni grades tend to be higher in the lower limb. A reserve has been estimated (AR 082812) at 4.9 million tons grading 0.72% Ni and 0.19% Cu. Up to several hundred ppm Co and 200 ppb Pd are present in selected samples. Pt values are rarely above a detection limit of 20 ppb."
075ESE0002,32,1,"The Dussault uranium prospect on the west shore of MacInnis Lake is situated within Aphebian sediments in the Nonacho Basin, an intermontane basin perched on Archean basement rocks of the Rae Province. Mineralization consists of stratabound veins, disseminations and aggregates of pitchblende that are restricted to a 10 m thick unit or zone of interbedded arkose and siltstone/shale, apparently within the Taltson Formation. Individual veins are up to 5 mm thick but are generally much narrower. Chloritic alteration is closely associated with pitchblende. Pyrite occurs in quartz and calcite stringers with pitchblende and also as disseminated cubes in the wall rocks. Other associated minerals include hematite, chalcopyrite and galena. Secondary U minerals are developed at the surface on high grade veins.  The main mineralized zone has been traced for 150 m along strike, to 60 m at depth and is generally between 0.5 and 2.0 m thick. Strike and dip are approximately 030 degrees and 50 degrees east respectively.  Mineralization rakes to the NNE at about 40 degrees. Canadian Pipelines and Petroleum Ltd. drilled 50 holes totalling 5194 m in the zone in 1955 - 56 and outlined 27,000 tonnes grading 0.17% U metal."
075ESW0001,33,1,"The OConnor Lake quartz vein-hosted sulphide deposit occurs in a medium to high grade metamorphic terrane within the Taltson magmatic arc. Lithologies in the general area of mineralization include metasediments, amphibolites, sillimanite-garnet gneiss and quartz-biotite schist. Numerous other quartz veins, some of which also contain base metal sulphides, are present in the area.  The MWK #1 vein cuts an amphibolite band where it is exposed at surface, trending northwesterly with a dip of 65 degrees to the southwest. Its width varies between 0.5 and 2 m and averages about 1.5 m. Its contacts are relatively sharp although minor quartz veins and stringers in the wall rocks, averaging 15 cm in thickness, parallel the main vein. A thin seam of graphite occurs at the footwall contact. Sphalerite and galena are disseminated throughout the quartz together with lesser pyrite and pyrrhotite. Pyrite and chalcopyrite are abundant locally. Larger masses of sphalerite and galena tend to occur near the vein margins and most exploration work has concentrated on several shoots of this material, which tend to pitch at 50 degrees to the northwest in the plane of the vein.  Drilling and underground drifting have traced the mineralized zone over 200 m in strike and to a depth of about 80 m. A drill-indicated reserve of 67,950 tons grading 7.64% Zn, 3.12% Pb, 0.13% Cu and 0.29 oz/ton Ag has been established."
075FSW0001,34,1,"The Salkeld Lake Cu-Ag occurrence is situated within the Nonacho Basin, an Aphebian intermontane basin perched on high grade Archean basement rocks of the Rae structural province. The Nonacho Group sediments comprise a sequence of freshwater clastic sediments including mainly arkose with lesser conglomerate, siltstone, shale and sandstone. All Aphebian rocks have been metamorphosed to the lower greenschist facies with development of phyllite and some granitization near intrusions. The area is intensely faulted and complexly folded, with many superimposed deformational events.  The immediate vicinity of the Salkeld Lake occurrence is underlain by banded biotitic granite gneiss which is cut by red granite to syenite. The red granite is commonly fractured and contains locally abundant milky white quartz veins constituting up to 50% of the rock. Unconformably overlying the gneiss/granites, are the lower three formations of the Nonacho Group comprising mainly conglomerate, arkose and greywacke.  Two mineralized zones occur at or near the contact between sediments and basement gneisses. The Stockwork Zone comprises fine disseminations and fracture-fillings of bornite and chalcopyrite near sheared zones in gneiss, arkose and conglomerate. Sheared zones are typically up to a metre wide, schistose and contain abundant malachite and azurite. Generally weak but locally intense silicification, biotitization and hematization are present as well as fracture-controlled fluorite. Anomalous elements include mainly Cu and Ag with lesser Zn, Pb, Mo, Bi and Au."
075FSW0001,35,2,"The Shear-Hosted Zone is a large zone of shearing, fracturing, silicification and quartz veining marking the contact between red granite and overlying sediments. It is exposed over more than 200 metres and is up to 40 metres wide locally. Disseminated chalcopyrite and bornite occur near the margins of higher-grade shears. Within the broad contact zone and sub-parallel to the granite-sediment contact, is a 10-30 metre wide sub-zone of intense quartz veining and silicification. Where this is intersected by shears, there are quartz breccias up to 5 metres wide mineralized with massive chalcocite and lesser amounts of bornite, sphalerite, chalcopyrite, galena and tetrahedrite. Smaller quartz veins locally containing clots of chalcopyrite together with fractures containing sphalerite, galena and chalcopyrite are also present.  Two minimum reserves based on earlier drilling were calculated by Fortune Minerals. A 150 ft wide portion of the Stockwork Zone was drilled on 50 ft centres and contains a reserve of 64,400 tons grading 0.63% Cu. A reserve of 59,000 tons grading 1.42% Cu and 1.74 oz/ton Ag was calculated for a 550 ft strike length of the Shear-Hosted zone to a depth of 100 ft."
075LNW0002,36,1,"The BBX Cu-Ag-Ni-Co prospect occurs in Aphebian Great Slave Supergroup rocks within the Great Slave Basin or Fold Belt. Copper mineralization is associated with a 1870+/-15 Ma basaltic diatreme, one of seven volcanic centres in the vicinity of Taltheilei Narrows that intrude sediments of the Great Slave Supergroup. The diatreme consists mainly of accidental fragments of mafic volcanics, and lesser sedimentary and granitic rocks set in a matrix of finely comminuted rock debris. Juvenile volcanic material is thought to represent less than 25% of the diatreme by volume.                      Mineralization at the BBX prospect is thought to be the result of several phases of activity. An early phase involved the deposition of Fe-Co-Ni sulphides and sulpharsenides such as gersdorffite, arsenopyrite and glaucodot. Later phases saw the deposition of chalcopyrite, galena, barite and specularite. These minerals occur as disseminations in the matrix of the diatreme, and in fractures and veinlets cutting both matrix and fragments. A last phase involved the development of quartz-carbonate veins.                      In general, the diatreme exhibits pervasive chloritic and carbonate alteration, both probably related to deuteric processes. Hematitic alteration took place at the time of emplacement. Potassic alteration involving the development of K-feldspar and sericite is intimately associated with metallic mineralization.  Work commenced on the BBX showing in 1948 when it was staked, trenched and diamond drilled. It was again drilled in 1956. From 1971-1974 the area was subjected to geological mapping, geochemical sampling, IP and magnetic geophysical surveys and diamond drilling. A resource was calculated at 5,000 t at 6.13% copper and 2.6 oz/t silver."
075LSW0001,37,1,"The Sachowia Lake Ni-Co-Bi deposit area is underlain by Archean Yellowknife Supergroup rocks, including mafic flows and fragmentals together with metasediments. A large granitic intrusion is present to the north; various small granite pegmatite and aplite dykes within the layered rocks are probably related to it. Ferruginous sediments and lava flows of the Kahochella Formation (Great Slave Supergroup) overlie Archean basement approximately 1 km south of the occurrences.  Niccolite, skutterudite, gersdorffite, rammelsbergite, arsenopyrite, pyrite and chalcopyrite occur in structurally controlled quartz-carbonate veins and vein breccias. The latter are generally less than 1 m in width but locally swell to 3 m. Metallic mineral content varies considerably within the veins, with one 1958 drill hole intersecting approximately 1 m of massive niccolite.  "
075MSE0001,38,1,"Regional: The Susu Lake Cu showing is situated within the Indian Mountain greenstone belt which comprises mainly Archean Yellowknife Supergroup supracrustal rocks. The belt is as much as 15 miles wide and extends 40 miles north from Great Slave Lake.  The belt is bounded on the east and west by granitic and migmatitic rocks but has a core of relatively low grade metamorphic rocks(Heywood and Davidson 1969).  The belt is seen to lie on deformed granitoid rocks in some places and in others to be intruded by granitic plutons of closely related age.  Property: The property in which this showing occurs, lies approximately 8 miles west of Susu Lake.  It comprises a volcanic belt that is part of the larger Indian Mountain greenstone belt.  The volcanic belt is dominated by rhyolites with quartz-biotite-cordierite schists.  Deformation in the area includes shearing and brecciation.  Intrusions of quartz veins are also noted.  Showing: The Susu Lake Cu showing occurs in a brecciated shear zone that hosts disseminated chalcopyrite and bornite.  Mineralization is largely hosted by rhyolites, but also occurs in neighboring quartz-biotite-cordierite schists.  Reserves were calculated at 142,500 tons grading 0.95% Cu in 1967 from 9 diamond drill holes that were drilled by Indian Mountain Metal Mines.  No other work on the showing has been recorded to date although in Canadian Mineral Deposits Not Being Mined in 1989, it was mentioned the property had been sold to Ego Resources.            "
075MSE0002,39,1,"The BB prospect is one of three related volcanogenic massive sulphide occurrences situated in the Indian Mountain greenstone belt in the southern Slave structural province. All stratified rocks have been mapped as belonging to the Archean Yellowknife Supergroup. The base of the stratigraphic sequence in the vicinity of the deposits comprises a series of mafic tuffs with minor, massive and pillowed mafic flows. The bottom of this unit is migmatized. Overlying this mafic base are intermediate tuffs and flows and then a felsic unit including massive rhyolite, intermediate to felsic coarse pyroclastics, tuff, lapilli tuff and tuff breccia. Sulphide deposits are hosted by a 1 - 10 metre thick unit of carbonate-rich exhalite and pyritic cherty tuff, overlying or near the top of the felsic unit. The stratigraphic succession is completed by greywackes and argillites. All stratified rocks have been metamorphosed to middle amphibolite facies.                      The BB massive sulphide deposit consists of a series of closely spaced lenses interbedded with and grading into ""highly altered siliceous limestone"" which is probably a carbonate-rich exhalite. Layers of coarse grained pyrite and sphalerite are interbedded with layers of coarse grained pyrite and bands of massive, fine-grained sphalerite. Galena occurs as small grains and blebs within massive pyrite and sphalerite and as rims on host rock fragments in the latter. Small blebs of chalcopyrite are scattered throughout the deposit. Associated metallic minerals include minor amounts of chalcopyrite, pyrrhotite, marcasite, magnetite and tetrahedrite.                       "
075MSE0002,40,2,"Reserves were calculated for the BB showing and several values were reported, increasing in tonnage as the number of drill holes increased.  By the end of 1952, over 23,000 feet total drilling on the property had been completed and reserves were calculated at 924,000 tons grading 10.3% Zn, 0.85% Pb and 3.45 oz/ton Ag.    The BB Lake Copper zone is situated within a discordant alteration pipe/stringer zone underlying the BB and Kennedy Lake stratiform mineralization. Chalcopyrite and pyrrhotite occur as stringers, layers and seams in two bands 8 - 13 metres wide and up to 200 metres long. Sulphides in the higher grade portions of these bands are accompanied by a black, unidentified amphibole. The alteration pipe within which this stringer mineralization is located is zoned.  An inner, intensely altered zone consists of garnet, anthophyllite, cummingtonite, cordierite, sericite and sillimanite in a less intensely altered envelope which is characterized more by biotite, quartz and chlorite.        "
075MSE0002,41,3,"Work on the BB showing began in 1948 when the property of which the showing lies was discovered for McAvoy and was optioned off to Hollinger Gold Mines.  Diamond drilling was started on the property the following year.  Over 15,825 feet of core was drilled and reserves were calculated at 270,000 tons of ore averaging 15.68% Zn, 1.67% Pb and 5.21 oz./ton Ag to a depth of 400 feet.  In 1951, under the ownership of Indian Mountain Metal Mines Ltd., reserves were re-calculated after drilling to the 800 foot horizon.  Information of the drilling program done in 1951, gave good enough results for another 25,000 feet of drilling to be proposed for the following year.  By the end of 1952, the BB zone had been drilled to the extent of 23,000 feet and the amount of reserves for the zone increased to 924,000 tons.  Plans were under consideration for underground development and mill construction for 1953, but were not implemented.  In 1965, extensive electromagnetic and magnetometer surveys were done by Indian Mountain Metals Mines Ltd. to re-examine the entire volcanic belt.  In 1966, drilling was done on anomalies that were outlined the year before in the Kennedy Lake area.  After 1966, no work on the BB zone has been reported.  The property went to lease in 1974 and in 1979 the property was optioned to Ego Resources.                         The Kennedy Lake Zone which lies under Kennedy Lake is described in AR 061728 as the western extension of the BB zone although it is separated from the latter by a barren zone.  The zone is not exposed at the surface although drilling outlined it to be 120 feet long with a maximum width of 21 feet.  The ore is similar in all respects to that of the BB zone.  Reserves for the Kennedy Lake zone were calculated at 43,000 tons grading 7.3% Zn, 1.1% Pb and 4.0 oz./ton Ag."
075MSE0039,42,1,"The Kennedy Lake West prospect is one of three related volcanogenic massive sulphide occurrences situated in the Indian Mountain greenstone belt in the southern Slave structural province. All stratified rocks have been mapped as belonging to the Archean Yellowknife Supergroup. The base of the stratigraphic sequence in the vicinity of the deposits comprises a series of mafic tuffs with minor, massive and pillowed mafic flows. The bottom of this unit is migmatized. Overlying this mafic base are intermediate tuffs and flows and then a felsic unit including massive rhyolite, intermediate to felsic coarse pyroclastics, tuff, lapilli tuff and tuff breccia.  The stratigraphic succession is completed by greywackes and argillites. All stratified rocks have been metamorphosed to middle amphibolite facies.  Mineralization of the Kennedy Lake West prospect occurs as chalcopyrite with minor amounts of silver and sphalerite.  The chalcopyrite is associated with amphibole and garnet rich bands of the volcanics and is disseminated in nature.  The mineralization can be traced discontinuously over 2,000 feet between BB Lake and Kennedy Lake.  Pyrrhotite and pyrite are associated with the chalcopyrite in the low grade sections at approximately a 1:1 ratio."
075MSE0039,43,2,"The Kennedy Lake West prospect is located on the VOO claims which were first staked by James McAvoy in 1951.  In 1952, 6 diamond drill holes were drilled on the VOO claims totalling 2,987 feet.  In 1959, trenching was carried out and 757 feet were drilled in 10 holes.  In 1965, Indian Mountain Metal Mines Ltd. located an anomaly under Kennedy Lake which they drilled into in 1966.   The drilling intersected a zone of low grade disseminated chalcopyrite up to 120 feet wide.  This Kennedy Lake West copper zone has been estimated to contain 1,000,000 tons grading 0.90% Cu over a length of 835 feet.    In 1966, Indian Mountain Metal Mines Ltd. optioned the VOO claims and drilled 9 holes and intersected the westward extension of the copper zone.  The claims subsequently lapsed and the ground was restaked by K. J. McDonald in May 1972 and later that month transferred to Indian Mountain Metal Mines Ltd.  Exploration work included geological mapping and a ground EM survey. Channel samples averaged 0.5% Cu and 0.94 oz./ton Ag over a width of 25 feet.    In 1974, a tonnage figure for the Kennedy Lake West zone was reported as 1,500,000 tons grading 0.62% Cu, including a higher grade core of 612,000 tons grading 1.12% Cu.  In 1979, Indian Mountain Metal Mines Ltd. amalgamated to form Initiative Explorations Inc.  The property was then optioned off to Domego Resources Ltd. in the early 1980's, who still held the claims in summer 1998."
076DNE0020,44,1,"The area is underlain by Archean greywacke, mica schists, and quartzite of the Yellowknife group intruded by Archean age granitic rocks.  Proterozoic diabase and gabbro dykes intrude the earlier Archean metasedimentary and granitic rocks.  Within the main claim block area kimberlite pipes are the only Phanerozoic age rocks known.  Minor amounts of metasedimentary rocks occur within the claim area and mostly comprise thinly bedded metagreywacke outcrops with small rafts of migmatite.  At least 5 types of granitoid intrusive rocks occur.  A large, homogeneous pluton of equigranular, medium grained quartz diorite occurs in the south-central portion of the main claim block and comprises plagioclase, biotite, hornblende, quartz and epidote.  The pluton is weakly deformed with poor foliation development.  Hornblende plus biotite tonalite and biotite tonalite are obseved to intrude the metagreywackes and have weak to strong foliations.  The two most voluminous granitoid rocks present in the main claims block area include a distinctive two mica granite and porphyritic biotite granite.  The two mica granite typically comprises equal proportions of quartz, plagioclase and potassium feldspar with 5 - 10% muscovite and biotite.  Apatite and tourmaline are common.  These granites are fine to medium grained and generally equigranular.  A tourmaline bearing pegmatitic phase forms dykes and small stocks up to 250 m in diameter.  The two mica granite intrudes greywacke and both tonalite units."
076DNE0020,45,2,"Diabase dykes are common in the main claims block area and post date the granitoid rocks.  Diabase dyke swarms present within the claim area include the McKay dyke, Contwoyto dyke swarm, Lac de Gras dykes, Mackenzie dyke swarm and 305 dykes.  At least 26 kimberlites have been discovered within the main claims area and post-date the granitoid rocks and diabase dykes.  The kimberlite pipes have undergone minimal erosion as evidenced by preservation of crater eqiclastic sediments.  The kimberlites are typically several hundred metres in diameter, occur within glacially formed lakes and are overlain by 5 to 30 m of sand and gravel.  Varieties of kimberlite distinguished in drill core inlcude epiclastic, tuffisitic and tuffisitic kimberlite breccia phases and massive hypabyssal kimberlite.  Glacial deposits are varied and include trunk and tributary esker ridges, drumlin-like boulder clay hills and till sheet(s).  Glacial erosion has rounded, grooved and polished the bedrock.  Till is the most common surficial sediment identified in the Lac de Gras area.  A single till sheet attributed to Late Wisconsinan Laurentide Ice represents several different directions of transport, including east to west, southeast to northwest and northeast to southwest.  Glaciofluvial deposits are also geographically widespread on the main claim block and are dominantly in the form of eskers and related kames.  The eskers range from small sinuous ridges to large more linear features up to 45 m high, forming the major topographic relief in the area."
076DNE0020,46,3,"The predominant rock type in the Fox area is a medium-grained biotite granite.  The rock is mostly unaltered but weak to moderate potassic alteration occurs at the east end of the ravine near the Fox portal and also along the swamp subparallel to the ravine.  Two diabase dykes cross the Fox Lake and were identified by an airborne magnetometer survey and in the decline and confirmed by small patches of outcrop located to the northeast and south of the lake.  Glacial sediments on the bottom of Fox Lake range from 15 to 25 metres thick and consist of silt and sand-sized particles of quartz, feldspar, biotite, epidote, amphibole and traces of kimberlite indicator minerals.  Gravel-sized rock fragments included various granitoid rocks.  Geophysical surveys and geochemical sampling was done over the Fox pipe.  In May, 1994 a decline-ramp/underground mining program was initiated to bulk sample the Fox kimberlite pipe.  When the underground bulk sampling program of the Fox pipe had been completed, 6,915 tonnes of kimberlite had been extracted.  The sample yielded 11,960 diamonds weighing 1,766 carats, for and overall grade of 0.26 carats per dry metric tonne.  The evalusation of the diamond parce returned an average of US $126.  Underground raises driven near the pipe periphery to a vertical height of 32 meters and near the pipe center to a height of 32 meters resulted in higher grade samples of 0.34 and 0.38 carats per dry metric tonne, respectively."
076DNE0020,47,4,"The Ekati project is held 51% by BHP Diamonds, 29% by Dia Met Minerals and the remaining 20% is split between Charles Fipke, the geologist who found diamonds in the NWT and Stewart Blusson, prospector and partner of Fipke. The mine plan for Ekati involves the development of the Panda, Misery, Koala, Sable and Fox pipes.  The Fox pipe will be subjected to open-pit mining from years 11 to 17.  Minable reserves are estimated at 16.7 million tonnes grading 0.4 carat at a value of US$125 per carat.  Fox Lake will be dewatered during the summer before preporduction commences in this pit, expected to be 2002, the sixth year of project development.  At a pumpling rate of approximately 1,600 cubic metres per hour it will take four months to pump out the 4.3 million cubic metres of water contained in the lake.  The turbid water and slimes encountered as the water level falls will be pumped to a natural containment area diked off with rock fill in the southern portion of the old Fox Lake bottom.  Excess water behind this impoundment will be discharged after solids settling or treatment brings the water quality below the discharge limits."
076DNE0021,48,1,"The area is underlain by Archean greywacke, mica schists, and quartzite of the Yellowknife group intruded by Archean age granitic rocks.  Proterozoic diabase and gabbro dykes intrude the earlier Archean metasedimentary and granitic rocks.  Within the main claim block area kimberlite pipes are the only Phanerozoic age rocks known.  Minor amounts of metasedimentary rocks occur within the claim area and mostly comprise thinly bedded metagreywacke outcrops with small rafts of migmatite.  At least 5 types of granitoid intrusive rocks occur.  A large, homogeneous pluton of equigranular, medium grained quartz diorite occurs in the south-central portion of the main claim block and comprises plagioclase, biotite, hornblende, quartz and epidote.  The pluton is weakly deformed with poor foliation development.  Hornblende plus biotite tonalite and biotite tonalite are obseved to intrude the metagreywackes and have weak to strong foliations.  The two most voluminous granitoid rocks present in the main claims block area include a distinctive two mica granite and porphyritic biotite granite.  The two mica granite typically comprises equal proportions of quartz, plagioclase and potassium feldspar with 5 - 10% muscovite and biotite.  Apatite and tourmaline are common.  These granites are fine to medium grained and generally equigranular.  A tourmaline bearing pegmatitic phase forms dykes and small stocks up to 250 m in diameter.  The two mica granite intrudes greywacke and both tonalite units."
076DNE0021,49,2,"Diabase dykes are common in the main claims block area and post date the granitoid rocks.  Diabase dyke swarms present within the claim area include the McKay dyke, Contwoyto dyke swarm, Lac de Gras dykes, Mackenzie dyke swarm and 305 dykes.  At least 26 kimberlites have been discovered within the main claims area and post-date the granitoid rocks and diabase dykes.  The kimberlite pipes have undergone minimal erosion as evidenced by preservation of crater eqiclastic sediments.  The kimberlites are typically several hundred metres in diameter, occur within glacially formed lakes and are overlain by 5 to 30 m of sand and gravel.  Varieties of kimberlite distinguished in drill core inlcude epiclastic, tuffisitic and tuffisitic kimberlite breccia phases and massive hypabyssal kimberlite.  Glacial deposits are varied and include trunk and tributary esker ridges, drumlin-like boulder clay hills and till sheet(s).  Glacial erosion has rounded, grooved and polished the bedrock.  Till is the most common surficial sediment identified in the Lac de Gras area.  A single till sheet attributed to Late Wisconsinan Laurentide Ice represents several different directions of transport, including east to west, southeast to northwest and northeast to southwest.  Glaciofluvial deposits are also geographically widespread on the main claim block and are dominantly in the form of eskers and related kames.  The eskers range from small sinuous ridges to large more linear features up to 45 m high, forming the major topographic relief in the area."
076DNE0021,50,3,"The predominant host rock type for the Koala pipe is a white to grey, medium to coarse-grained, weakly foliated to massive biotite granite.  The granite locally contains rounded biotite-rich mafic xenoliths.  A variety of other rock types exist including granodiorite, granite gneiss and small patches of diorite.  The granite gneiss, observed about 80 m SE of the lake, contains traces to 1% almandine garnets that are 1 to 2 mm in size and form circular pods up to 3.5 cm diameter.  Also within the gneiss are rare occurrences of tabular tourmaline crystals up to about 2 cm in length.  The diorite, scattered throughout the area to the east jof Koala Lake, contains traces of almandine garnet and traces of disseminated sulphides.  The bottom of Koala Lake and the Koala kimberlite pipe are covered by unconsolidated sediments of glacial origin.  This overburden is characterized by a complex interfingering of sediments lenses ranging from mud to gravel.  Generally the uppermost part of the overburden sequence comprises well sorted silt and mud.  Elsewhere sand and gravel dominate.  In most cases, fine clay and silt have been washed and weathered out of these coarse grained sediments.  Boulders and cobbles are sporadic throughout the sequence."
076DNE0021,51,4,"The Ekati project is held 51% by BHP Diamonds, 29% by Dia Met Minerals and the remaining 20% is split between Charles Fipke, the geologist who found diamonds in the NWT and Stewart Blusson, prospector and partner of Fipke. The mine plan for Ekati involves the development of the Panda, Misery, Koala, Sable and Fox pipes.  It is expected that the Koala pipe will be mined by open pit methods from years 5 to 11 and by underground methods from years 11 to 15.  Minable pit reserves are estimated at 14.6 million tonnes grading 0.76 carat, underground reserves at 2.8 million tonnes grading 1.63 carat.  The diamonds are valued at US$122 per carat."
076DNE0022,52,1,"The area is underlain by Archean greywacke, mica schists, and quartzite of the Yellowknife group intruded by Archean age granitic rocks.  Proterozoic diabase and gabbro dykes intrude the earlier Archean metasedimentary and granitic rocks.  Within the main claim block area kimberlite pipes are the only Phanerozoic age rocks known.  Minor amounts of metasedimentary rocks occur within the claim area and mostly comprise thinly bedded metagreywacke outcrops with small rafts of migmatite.  At least 5 types of granitoid intrusive rocks occur.  A large, homogeneous pluton of equigranular, medium grained quartz diorite occurs in the south-central portion of the main claim block and comprises plagioclase, biotite, hornblende, quartz and epidote.  The pluton is weakly deformed with poor foliation development.  Hornblende plus biotite tonalite and biotite tonalite are obseved to intrude the metagreywackes and have weak to strong foliations.  The two most voluminous granitoid rocks present in the main claims block area include a distinctive two mica granite and porphyritic biotite granite.  The two mica granite typically comprises equal proportions of quartz, plagioclase and potassium feldspar with 5 - 10% muscovite and biotite.  Apatite and tourmaline are common.  These granites are fine to medium grained and generally equigranular.  A tourmaline bearing pegmatitic phase forms dykes and small stocks up to 250 m in diameter.  The two mica granite intrudes greywacke and both tonalite units."
076DNE0022,53,2,"Diabase dykes are common in the main claims block area and post date the granitoid rocks.  Diabase dyke swarms present within the claim area include the McKay dyke, Contwoyto dyke swarm, Lac de Gras dykes, Mackenzie dyke swarm and 305 dykes.  At least 26 kimberlites have been discovered within the main claims area and post-date the granitoid rocks and diabase dykes.  The kimberlite pipes have undergone minimal erosion as evidenced by preservation of crater eqiclastic sediments.  The kimberlites are typically several hundred metres in diameter, occur within glacially formed lakes and are overlain by 5 to 30 m of sand and gravel.  Varieties of kimberlite distinguished in drill core inlcude epiclastic, tuffisitic and tuffisitic kimberlite breccia phases and massive hypabyssal kimberlite.  Glacial deposits are varied and include trunk and tributary esker ridges, drumlin-like boulder clay hills and till sheet(s).  Glacial erosion has rounded, grooved and polished the bedrock.  Till is the most common surficial sediment identified in the Lac de Gras area.  A single till sheet attributed to Late Wisconsinan Laurentide Ice represents several different directions of transport, including east to west, southeast to northwest and northeast to southwest.  Glaciofluvial deposits are also geographically widespread on the main claim block and are dominantly in the form of eskers and related kames.  The eskers range from small sinuous ridges to large more linear features up to 45 m high, forming the major topographic relief in the area."
076DNE0024,54,1,"The area is underlain by Archean greywacke, mica schists, and quartzite of the Yellowknife group intruded by Archean age granitic rocks.  Proterozoic diabase and gabbro dykes intrude the earlier Archean metasedimentary and granitic rocks.  Within the main claim block area kimberlite pipes are the only Phanerozoic age rocks known.  Minor amounts of metasedimentary rocks occur within the claim area and mostly comprise thinly bedded metagreywacke outcrops with small rafts of migmatite.  At least 5 types of granitoid intrusive rocks occur.  A large, homogeneous pluton of equigranular, medium grained quartz diorite occurs in the south-central portion of the main claim block and comprises plagioclase, biotite, hornblende, quartz and epidote.  The pluton is weakly deformed with poor foliation development.  Hornblende plus biotite tonalite and biotite tonalite are obseved to intrude the metagreywackes and have weak to strong foliations.  The two most voluminous granitoid rocks present in the main claims block area include a distinctive two mica granite and porphyritic biotite granite.  The two mica granite typically comprises equal proportions of quartz, plagioclase and potassium feldspar with 5 - 10% muscovite and biotite.  Apatite and tourmaline are common.  These granites are fine to medium grained and generally equigranular.  A tourmaline bearing pegmatitic phase forms dykes and small stocks up to 250 m in diameter.  The two mica granite intrudes greywacke and both tonalite units."
076DNE0024,55,2,"Diabase dykes are common in the main claims block area and post date the granitoid rocks.  Diabase dyke swarms present within the claim area include the McKay dyke, Contwoyto dyke swarm, Lac de Gras dykes, Mackenzie dyke swarm and 305 dykes.  At least 26 kimberlites have been discovered within the main claims area and post-date the granitoid rocks and diabase dykes.  The kimberlite pipes have undergone minimal erosion as evidenced by preservation of crater eqiclastic sediments.  The kimberlites are typically several hundred metres in diameter, occur within glacially formed lakes and are overlain by 5 to 30 m of sand and gravel.  Varieties of kimberlite distinguished in drill core inlcude epiclastic, tuffisitic and tuffisitic kimberlite breccia phases and massive hypabyssal kimberlite.  Glacial deposits are varied and include trunk and tributary esker ridges, drumlin-like boulder clay hills and till sheet(s).  Glacial erosion has rounded, grooved and polished the bedrock.  Till is the most common surficial sediment identified in the Lac de Gras area.  A single till sheet attributed to Late Wisconsinan Laurentide Ice represents several different directions of transport, including east to west, southeast to northwest and northeast to southwest.  Glaciofluvial deposits are also geographically widespread on the main claim block and are dominantly in the form of eskers and related kames.  The eskers range from small sinuous ridges to large more linear features up to 45 m high, forming the major topographic relief in the area."
076DSW0001,56,1,"The Deb volcanogenic massive sulphide deposit is located in the Courageous - Mackay Lake greenstone belt in the Slave structural province.  The belt runs north-south, dips steeply to the east and is composed of Yellowknife Supergroup volcanics.  In the east they are overlain by Yellowknife Supergroup sediments and in the west are assimilated from below by granites.  The Deb deposit is contained within a series of volcanics of varying composition but seems most closely related to felsic pyroclastics.  Around the showing sub-volcanic gabbroic intrusions have disrupted the volcanics.  Massive sulphides are situated within the lower felsic unit and include massive pyrrhotite, pyrite and sphalerite underlain by stringers of chalcopyrite and pyrrhotite. The latter are accompanied by strong chloritization, biotitization, sericitization and garnets in a small but well-developed alteration pipe/stringer zone underlying the stratiform mineralization.  The mineralized horizon is relatively undeformed and has been traced by drilling over an 800 metre strike length, to a depth of 230 metres and has an average width of 3.8 metres.  Mineral zonation is recognizable in both a vertical and lateral sense with respect to stratigraphy.  Zinc is prominent at the stratigraphic top of the zone gradually giving way to a copper rich section.  Galena is generally more abundant within the zinc rich portions."
076DSW0001,57,2,"Drilling in 1979 (assessment report 081299) was successful in delineating the zone of copper-zinc mineralization.  There were 3 holes drilled in 1980.  One hole tested the gravity anomaly below the deposit and found it was due to a large gabbro body.  The 2 other holes were drilled to test the deposit at depth.  Core samples were assayed for gold, silver, copper, lead and zinc.  Results from assaying returned values to 7.21% zinc, 2.76% copper, 2.36 oz/T silver and 1.04% lead.  The 1986-87 Mineral Industry Report for the Northwest Territories reports that drill testing of the Deb deposit indicated 1,015,000 t containing 0.83% copper, 2.96% zinc and 21.9 ppm silver.  The Canadian Mineral Deposits Not Being Mined in 1989 reports 1,118,000 tons at 0.83% copper, 2.96% zinc and 0.64 oz/T silver."
076DSW0002,58,1,"The Perrson Vein, BS or TK prospect, is located in the Courageous-Mackay Lake greenstone belt in the Slave structural province. It is hosted by a volcanosedimentary sequence belonging to the Archean Yellowknife Supergroup. The general area of the deposit is underlain by a stratigraphic sequence including, from oldest to youngest: mafic flows with minor tuff, mafic tuffs, a mixed unit of thinly-bedded and alternating mafic and felsic tuffs, felsic tuff and then clastic sediments. Metamorphic grade at the prospect is greenschist facies.  Two auriferous zones, the Perrson and East Perrson zones, occur as seperate stratabound horizons in the felsic tuff unit immediately below its contact with the overlying sediments. Mineralization consists of 1 - 3% finely disseminated pyrite and finely acicular needles of arsenopyrite in a very fine grained, sericitic felsic tuff with intercalated cherty layers and/or narrow quartz veins. The Persson horizons vary in width from a few centimetres to 3 m. Quartz veins and/or cherty layers are generally conformable to foliation but locally exhibit tight folding or ptygmatic character.  A third zone, the Saucer Lake Zone, appears to be hosted by the mixed unit and consists of a horizon characterized by dark grey to milky quartz veins ranging in width from 1 cm to 1 m. The veins are variable in orientation, exhibiting both cross-cutting and conformable relationships and do not contain sulphides. Arsenopyrite and pyrite occur as clots and crystals in altered wall rock inclusions in the quartz, the arsenopyrite also occurring in the wall rocks. In places, the arsenopyrite appears crudely banded or layered."
076DSW0002,59,2,"Drill logs from the Bow Valley work (AR 082546) describe alteration in the wall rock as strong chloritization with patches of hornblende.  The Perrson and East Perrson Zones have been traced by drilling over lengths of several hundred to one thousand metres and to a depth of about 125 m. Two drill-hole pierce points somewhat below a depth of 200 m show that, at least in these areas, mineralization does not continue to that depth. The Saucer Lake zone has been traced by drilling over a strike length of about 350 m.  Drilling in 1958 by North Goldcrest Mines Ltd. outlined a mineralized zone 950 feet in length, averaging 0.51 oz/ton gold over an average width of 2.2 feet.  The best intersections included 1.54 oz/T gold over 7 feet, 1.48 oz/T gold over 1.3 feet and 0.62 oz/T gold over 2 feet.  In 1983 Roxwell Gold Mines Ltd., using the 1958 drill results, calculated ore reserves for the Perrson Zone to be 37,500 tons proven and 75,000 tons probable with a weighted graded average of between 0.13 to 0.15 oz/T gold.  (NMI 076D03AU_06)  The initial gold showings on the BS claims were discovered in 1945.  Homer Yellowknife Mines conducted limited diamond drilling in 1947 and 1949 with the first 7 holes testing the Perrson and East Perrson veins.  All holes encountered gold mineralization.  The property was subsequently acquired by Goldcrest Mines Ltd. who conducted some mapping and drilling.  In 1970 the claims were restaked and optioned to Perry River Nickel Mines in 1974.  The option terminated in 1978.  The claims lapsed and were restaked and optioned to Roxwell Gold Mines Ltd. in 1981.  In 1983 Giant Yellowknife Mines Ltd. acquired an option on the property.  In 1987 Bow Valley Industries Ltd. entered an option agreement with Roxwell Gold Mines."
076DSW0003,60,1,"The Tundra deposit, also known as Fat, is located in the Courageous-Mackay Lake greenstone belt in the Slave structural province. All stratified rocks have been mapped as belonging to the Archean Yellowknife Supergroup and have been metamorphosed to the greenschist facies.  Two separate gold-bearing zones are present in a volcanic sequence known as the Matthews Lake Volcanic Complex which has been divided into a lower and upper cycle. The lower cycle comprises a 400 metre thick unit of rhyodacitic flows overlain by 45 - 150 metres of interbedded calcareous sediments and calcareous rhyodacitic lapilli tuff, and capped by a narrow layer of locally graphitic pelite. The base of the upper cycle comprises a 180 - 300 metre thick unit of rhyodacitic lapilli tuff to agglomerate, overlain by felsic volcanics transitional to typical Yellowknife Supergroup sediments.  The largest auriferous zone, known as the Tundra or Fat zone, occurs in felsic volcanics of the upper cycle. It is a 100 - 250 metre wide zone consisting of multiple, parallel, subvertically dipping shear zones that are subparallel to strata. Individual shears range from 3 - 20 metres in thickness and are characterized by variable but generally strong sericitization, silicification, chloritization and irregular blue-grey to dark grey quartz veins and masses. Many of the latter have diffuse boundaries. Very finely acicular arsenopyrite is the main sulphide mineral, occurring as disseminations throughout the sericitized rock and as felted masses. Lesser pyrrhotite and pyrite occur as disseminations. Chalcopyrite, sphalerite and scheelite have been identified within the zones but are rare. Gold is largely refractory, being tied up within arsenopyrite."
076DSW0003,61,2,"However, a significant proportion occurs as free metal in extremely fine grains averaging less than 10 microns in size. Some of these occur in fractures or inclusions in arsenopyrite but the majority is interstitial to silicates. Visible gold is rare and seen only in some quartz veins.  The Tundra zone has been traced with drilling over a 1500 metre strike length and locally to a depth of 1300 metres. It is open to depth. A 476 metre vertical shaft was sunk in 1988-89 and 2000 metres of underground development on the 425m level were completed. In 1989, the Noranda-Hemlo-Total Energold joint venture announced suspension of the project because of the relatively low gold grade.  A report prepared by Noranda in 1990 estimates the total geological reserves for the Tundra deposit at 15.47 million metric tonnes grading 6.5 grams per tonne above a 3.4 gram cut-off.  In 1990 a limited surface exploration program was carried out.  The Carbonate zone is not well described in available literature. It occurs at the contact between felsic volcanics and overlying pelites in the lower cycle. It apparently resembles the Salmita Mine host rock. A reserve of 900,000 tonnes grading 12 g/t Au is quoted in the 1986-87 DIAND MIR (p265)."
076DSW0004,62,1,"The Jax Lake gold deposit is situated within the Courageous-Mackay Lake greenstone belt in the Slave structural province. All stratified rocks have been mapped as belonging to the Archean Yellowknife Supergroup and have been metamorphosed to the lower greenschist facies except at the north end of Jax Lake, where the presence of cordierite indicates lower amphibolite facies.                      The stratigraphic sequence in the deposit area has been divided into two cycles. The lower cycle begins with massive mafic flows successively overlain by banded mafic tuffs, felsic flows and tuffs, banded mafic tuffs and then graphitic chert. The upper cycle begins with massive mafic flows, followed by well-banded and carbonate-rich mafic tuffs, porphyritic massive felsic volcanics and finally metasediments. Large sills and dykes of metagabbro and metadiorite tend to occur at the contact between the lower banded mafic tuffs and overlying mafic flows but are not restricted to this interval.                      Five auriferous zones have been identified in a long history of work in this area. The No. 1 zone strikes northerly, dips vertically or steeply to the east and consists of a number of light grey to blue-gray quartz veins and stringer zones at the contact between banded mafic tuffs and underlying massive flows in the upper cycle. Small amounts (less than 10%) of sulphide minerals occur in both the veins and adjacent wall rocks, including arsenopyrite, pyrrhotite, pyrite and lesser chalcopyrite. Alteration in and around the veins includes epidote, carbonate and sericite. Inclusions of altered wall rock in the veins are ubiquitous and some zones contain black tourmaline. Fine to coarse visible gold is scattered throughout the quartz."
076DSW0004,63,2,"Two main veins about 8 metres apart were traced along a strike length of about 80 metres. A reserve of 36,300 tonnes grading 14.06 g/t Au has been reported for this zone (VSE SMF for Perry River Nickel Mines 9/18/80).  The No. 2 zone may be the faulted-off southern extension of the No. 1 vein and occurs in a similar geological setting. Gold values are concentrated on the hangingwall side. Drilling has traced this vein over a strike length of 58 metres and shown it to grade 39.8 g/t Au over an average width of 0.91 metres.  The No. 3 zone is situated within massive mafic volcanics stratigraphically below the No. 1 and 2 zones. Three parallel veins and stringers are present in a 6.5 metre wide zone. Bluish-gray to black quartz carries up to 5% pyrite, pyrrhotite and arsenopyrite. Surface samples have returned only trace to low values of gold.  The No. 4 zone consists of a number of quartz veins parallelling schistocity that are situated about 60 metres higher in the stratigraphy than the other zones. Both pyrrhotite and arsenopyrite are present in the veins, the arsenopyrite also occurring locally in the wall rock as coarse crystals. Of six samples collected across 6.5 metres, the best graded 10.6 g/t Au over 0.7 m. A shallow hole drilled under the outcrop in 1946 cut 2.5 feet of quartz grading 0.09 oz/ton Au.  A fifth zone is plotted on a 1960 geology map in AR 017118 and discussed in AR 062023. This is probably the Sour Lake occurrence which has its own entry in this database."
076DSW0020,64,1,"The Perrson Vein, BS or TK prospect, is located in the Courageous-Mackay Lake greenstone belt in the Slave structural province. It is hosted by a volcanosedimentary sequence belonging to the Archean Yellowknife Supergroup. The general area of the deposit is underlain by a stratigraphic sequence including, from oldest to youngest: mafic flows with minor tuff, mafic tuffs, a mixed unit of thinly-bedded and alternating mafic and felsic tuffs, felsic tuff and then clastic sediments. Metamorphic grade at the prospect is greenschist facies.  Two auriferous zones, the Perrson and East Perrson zones, occur as seperate stratabound horizons in the felsic tuff unit immediately below its contact with the overlying sediments. Mineralization consists of 1 - 3% finely disseminated pyrite and finely acicular needles of arsenopyrite in a very fine grained, sericitic felsic tuff with intercalated cherty layers and/or narrow quartz veins. The Persson horizons vary in width from a few centimetres to 3 m. Quartz veins and/or cherty layers are generally conformable to foliation but locally exhibit tight folding or ptygmatic character.  A third zone, the Saucer Lake Zone, appears to be hosted by the mixed unit and consists of a horizon characterized by dark grey to milky quartz veins ranging in width from 1 cm to 1 m. The veins are variable in orientation, exhibiting both cross-cutting and conformable relationships and do not contain sulphides. Arsenopyrite and pyrite occur as clots and crystals in altered wall rock inclusions in the quartz, the arsenopyrite also occurring in the wall rocks. In places, the arsenopyrite appears crudely banded or layered."
076DSW0020,65,2,"Drill logs from the Bow Valley work (AR 082546) describe alteration in the wall rock as strong chloritization with patches of hornblende.  The Perrson and East Perrson Zones have been traced by drilling over lengths of several hundred to one thousand metres and to a depth of about 125 m. Two drill-hole pierce points somewhat below a depth of 200 m show that, at least in these areas, mineralization does not continue to that depth. The Saucer Lake zone has been traced by drilling over a strike length of about 350 m.  Drilling in 1958 by North Goldcrest Mines Ltd. outlined a mineralized zone 950 feet in length, averaging 0.51 oz/ton gold over an average width of 2.2 feet.  The best intersections included 1.54 oz/T gold over 7 feet, 1.48 oz/T gold over 1.3 feet and 0.62 oz/T gold over 2 feet.  In 1983 Roxwell Gold Mines Ltd., using the 1958 drill results, calculated ore reserves for the Perrson Zone to be 37,500 tons proven and 75,000 tons probable with a weighted graded average of between 0.13 to 0.15 oz/T gold.  (NMI 076D03AU_06)  The initial gold showings on the BS claims were discovered in 1945.  Homer Yellowknife Mines conducted limited diamond drilling in 1947 and 1949 with the first 7 holes testing the Perrson and East Perrson veins.  All holes encountered gold mineralization.  The property was subsequently acquired by Goldcrest Mines Ltd. who conducted some mapping and drilling.  In 1970 the claims were restaked and optioned to Perry River Nickel Mines in 1974.  The option terminated in 1978.  The claims lapsed and were restaked and optioned to Roxwell Gold Mines Ltd. in 1981.  In 1983 Giant Yellowknife Mines Ltd. acquired an option on the property.  In 1987 Bow Valley Industries Ltd. entered an option agreement with Roxwell Gold Mines."
076ENE0001,66,1,"The Butterfly deposit is in the Contwoyto-Itchen-Point Sedimentary Terrane, a large arcuate belt of Archean turbiditic metasediments belonging to the Yellowknife Supergroup, and affected by polyphase Archean deformation and regional metamorphism. The sedimentary belt is flanked to the west by the older, predominantly volcanic Point Lake supracrustal belt, and invaded to the east and north by late Archean granitoids. Late Proterozoic diabase dykes cut the supracrustals and the granites.  The sediments in the showing area are (garnet-staurolite)-cordierite-quartz-muscovite-biotite schists, the lower amphibolite grade equivalents of interbedded and graded-bedded argillites and subordinate greywackes. They are mostly fine-grained and micaceous, less commonly siliceous, and rarely graphitic. Cordierite is usually porphyroblastic, rarely incipient or absent, and often replaced by sericite/muscovite. The cordierite isograd is well to the west but dips shallowly east under the deposit. The sillimanite isograd, marking a further rise in grade to middle amphibolite, is immediately east of the deposit. Staurolite porphyroblasts are infrequent in the showing area, andalusite is rare, and garnet occurs near iron formations. Bedding strikes 120 - 140 degrees and dips 45 - 80 degrees SW in the deposit area.  Discontinuous lenses and layers of amphibolitic iron formation are interbedded with the clastic sediments. They are laminated or crudely banded to massive, with garnet-rich layers, cherty bands or pyrrhotite defining the layering."
076ENE0001,67,2,"From limited drill data submitted with assessment reports, the Butterfly deposit is hosted by a discontinuous lens of amphibolitic iron formation which breaks up along strike into numerous narrow bands, interdigitating and intergradational with the clastics, and farther NW along strike becomes a coherent unit of significant width again. Its strike length is apparently almost 400 m, and it has been intersected at 60 m depth. Core lengths of auriferous intersections range from 1 to 5 m. Reserves have been estimated at 100,000 tonnes grading 17 g/t Au, and it is open at depth.  Two diabase dykes cut the Butterfly iron formation, one trending NW and the other E.  The dominant schistocity is subparallel to bedding, and secondary crenulation cleavages are common. Complex folding is recorded in the compositional banding of the host iron formation."
076ENE0002,68,1,"The showing is in the Contwoyto-Itchen-Point Sedimentary Terrane, a large arcuate belt of Archean turbiditic metasediments of the Yellowknife Supergroup, affected by polyphase Archean deformation and regional metamorphism. It is flanked to the west by the older, predominantly volcanic Point Lake supracrustal belt, and invaded to the east and north by late Archean granitoids. Late Proterozoic diabase dykes cut the supracrustals and the granites.  Little information is available on the deposit, due primarily to a conflict over ownership. It is probably a typical Contwoyto-type, iron formation-hosted gold deposit. The host sediments are cordierite-quartz-muscovite-biotite schists, the lower amphibolite grade equivalents of interbedded and graded-bedded argillites and greywackes. They range from fine-grained and micaceous to siliceous, and are locally graphitic. They host conformable layers and lenses of amphibolitic iron formation, commonly banded, and locally sulphidic with pyrrhotite, pyrite and arsenopyrite being the most common sulphides. Gold is assocaited with both quartz and sulphides in the iron formation units across the Lupin area.  From drill hole locations, limited drill log information, and AEM data, the deposit is 500 - 1000 m long, 2 - 4 m thick, strikes WNW and dips steeply north or south. It is probably contorted or folded, as are most of the iron formation units in the area. It is said to be a significant deposit (NMI).  A series of granitic sills, probably of late Archean age, intrude the schists at depth toward the east end of the deposit horizon (about 1 km E of inferred deposit location and DDH 88-57); narrow granitic dykes were intersected elsewhere.  A couple of NW-trending diabase dykes probably cut the Jon horizon."
076ENW0004,69,1,"The showing is in the Contwoyto-Itchen-Point Sedimentary Terrane, a large arcuate belt of Archean turbiditic metasediments of the Yellowknife Supergroup, affected by polyphase Archean deformation and regional metamorphism. It is flanked to the west by the older, predominantly volcanic Point Lake supracrustal belt, and invaded to the east and north by late Archean granitoids. Late Proterozoic diabase dykes cut the supracrustals and the granites.  The Pan deposit is hosted by a roughly tabular, NW-striking, moderately NE-dipping iron formation, enclosed by massive to finely bedded, foliated metagreywackes with slatey, argillaceous interbeds. Numerous thin, discontinuous layers of iron formation are interbedded with the clastics up to 200 m either side of the Pan horizon. Within a hundred metres south of the deposit the greywackes grade into more siliceous clastics mapped as siltstones. A couple of hundred metres west of the deposit, metamorphic grade rises from upper greenschist to lower amphibolite, marked by the appearance of cordierite nodules and increasing schistocity in the sediments. The cordierite isograd runs NW here and dips shallowly NE.  Intrusion of a 2 x 2 km, late Archean syenitic plug, which terminates the southern extent of the Pan horizon 60 m SE of the last drill intersection, caused micaceous hornfels metamorphism of the sediments and localized intrusive deformation. Two syenite dykes 2 - 3 m wide strike NE through the Pan horizon. A Helikian diabase dyke trends NNW about 150 m south of the Pan."
076ENW0004,70,2,"The host unit is a silicate-(sulphide) facies, quartz-garnet-amphibole iron formation. It is 2 - 6 m thick and auriferous along 180 m. Auriferous intersections 300 m and 780 m on strike to the NW may derive from the same horizon; exposure is so poor this cannot be verified. The Pan iron formation is compositionally banded, hosting Au-poor, garnet- rich layers, and Au-rich, pyrrhotite-rich, garnet-poor layers, and up to 50% disseminated to semi-massive arsenopyrite. A 1984 average grade is based on 8 holes, on 40 m centres testing 20 m and 50 m vertical depths along 183 m, and is 2.8 g/t Au across an average true width of 3.2 m."
076ENW0005,71,1,"The deposit lies within the Central Volcanic Belt, an E-striking, N-dipping and -facing sequence of mixed mafic to felsic volcanics belonging to the Point Lake Formation of the Archean Yellowknife Supergroup. Two cycles of volcanism have been tentatively suggested (Bubar and Heslop, 1985). The volcanic belt is bounded to the north by clastic metasediments of the Yellowknife Supergroup (Itchen and Contwoyto Formations), and to the south by mixed granitoids, in part pre-Yellowknife Supergroup basement. Small, late Archean granitic plutons and pegmatite dykes locally intrude the supracrustals.  A unit of massive mafic flows with minor intercalated tuffaceous horizons forms the base of the volcanic pile. Overlying this is a 500 metre thick sequence of intermediate to felsic fragmental and volcaniclastic rocks, including the chloritized tuffs and lapilli tuffs which host the deposit 250 m above the basal mafic flows. Above the host sequence is a predominantly felsic volcanic unit, separated from a presumed second volcanic cycle 2km NW of the deposit by a 1km-wide, fault-bounded band of metaturbidites.                      The immediate footwall to the deposit comprises felsic ash and lapilli tuffs, with minor coarser material and local thin intermediate beds. The immediate hangingwall is similar but contains a much greater proportion of coarse felsic volcaniclastics, including matrix-supported breccias interpreted as debris flows. A thin but distinctive pyrite-rich, quartz-sericite schist occurs at the hangingwall contact with the massive sulphides.                       The deposit itself is a stratiform, L-shaped body of well-banded, massive to disseminated sulphides. It lies in the NE-striking, synformal hinge zone of a regional, open Z-fold, and comprises two steeply dipping to vertical limbs striking at 170 degrees and 080 degrees."
076ENW0005,72,2,"It is up to 40 m true thickness in the hinge zone, thins rapidly away from the hinge, but apparently widens with depth along the north limb where good grades were intersected. Pyrite and sphalerite are the dominant sulphides, accompanied by variable amounts of galena and chalcopyrite, and minor amounts of other metallic minerals. The central portions of the deposit tend to be enriched in Zn, Ag and Pb while outlying areas are relatively Cu-rich. Although the deposit is also vertically zoned, with Cu grades increasing toward the footwall, no significant stringer zone/alteration pipe has been found to date. The main mineralized zone in the fold hinge is primarily a Zn-Ag deposit.  Drill-indicated reserves in 1991 (Northern Miner Dec 09/91) were 7.3 million tonnes grading 4.8% Zn and 46 g/t Ag, with 0.2% Cu. Up to 2.8 g/t Au is reported locally.                      Chloritization is the most wide-spread alteration, comprising chlorite-pyrite ? cordierite ? garnet, in semi-conformable zones adjacent to the deposit and in fracture-controlled zones higher up the hangingwall. Sericitization is less wide-spread and comprises mainly quartz-muscovite-sericitized feldspar ? pyrite. A third alteration type, chlorite-cordierite-biotite or CBC, is most distinctive, occurring in contact with the sulphide mineralization irregularly along both hangingwall and footwall in zones up to 5 m wide. It comprises coarse-grained, well-foliated, dark-colored biotite-quartz-chlorite-cordierite (pyrite-chalcopyrite-sphalerite). A later metasomatic bleaching, characterized by quartz, K-feldspar and epidote, is locally superimposed on the above assemblages.                      The area has been affected by two folding episodes, the later one possibly related to shearing and formation of the open Z-fold hosting the deposit."
076ENW0005,73,3,"Two episodes of brittle deformation, the earlier definitely pre-pegmatite and possibly coinciding with synvolcanic tectonic activity and sulphide deposition (Bubar and Heslop, CIMM Bull Apr/85), have marked the Gondor locality with numerous, steeply dipping faults. Microfaulting and shearing have been noted in drill core and on surface. Two regional, NE-striking Proterozoic? faults occur about 2 km NW of the deposit."
076FNE0001,74,1,"The Hackett River occurrences, also known as the Bathurst Norsemines occurrences, include a number of volcanogenic massive sulphide lenses hosted by metavolcanics and metasediments of the Archean Yellowknife Supergroup in the Hackett River greenstone belt. Mineralization generally occurs in a mixed package of rhyolitic fragmentals, epiclastics, chemical and clastic sediments known as the Mineral Horizon sandwiched between a thick underlying sequence of fragmental rhyolites and overlying clastic sediments. Three main areas of mineralization have been described. The Central area includes the A, Jo and Jo South zones while the Boot Lake and East Cleaver areas occur at distances of 2 and 6 kilometres respectively. In the Central area, the A and Jo deposits are situated on a common stratigraphic horizon and consist of conformable lenses of pyrite with lesser sphalerite, galena and chalcopyrite. Both overlie discordant, zoned alteration pipe/stringer zones containing chalcopyrite, pyrrhotite, pyrite and magnetite. Alteration consists of a sericite - quartz - (sillimanite - cordierite) assemblage developed along hydrothermal fluid channelways, interspersed with patchy anthophyllite - cordierite - biotite - garnet - quartz - (sillimanite - sericite). Both are contained within a relatively wide envelope of characteristically spotted sillimanite - biotite - garnet - quartz - (cordierite - sericite) rock. The Jo South zone occurs at a lower stratigraphic level and comprises a series of veins and disseminations of pyrite, sphalerite, chalcopyrite and galena. The Boot Lake zone also occurs within the Mineral Horizon although the latter is thinner in this area, with a less complex internal stratigraphy. Sulphides are present in small lenses and in continuous layers of pyrite, both containing variable amounts of pyrrhotite, sphalerite, galena and chalcopyrite."
076FNE0001,75,2,"The East Cleaver zone is a single, fairly homogeneous sulphide body containing pyrite, sphalerite and galena, also situated within the Mineral Horizon. It has been deformed through folding and shearing and is now highly contorted, occupying the nose of an overturned anticline. Both zones are underlain by a stringer zone/alteration pipe similar to those under the A and Jo deposits.  A total reserve for the four zones is reported to be 21 million tons grading 4.98% Zn, 0.75% Pb, 0.41% Cu, 4.37 oz/ton Ag and 0.013 oz/ton Au (Northern Miner, 2/21/80)."
076GNE0017,76,1,"The Goose Lake showing lies within the northeastern portion of the Archean Slave Structural Province. The region is bordered by the Aphebian age Bear Structural Province to the west, and the Rae Structural Province to the east. The principal underlying supracrustal rocks belong to the Archean Yellowknife Supergroup and consist mainly of volcanics and metasediments. Archean intrusive and metamorphic rocks also underlie the region. Early Proterozoic (Aphebian) clastic sedimentary and carbonate sequences of the Goulburn Group unconformably overlie the Archean rocks locally. Intrusive rocks of Hudsonian age and younger diabase dykes crosscut the older lithologies.  The Goose Lake area is within the Back River region. The Yellowknife Supergroup in the property area is divided informally into three major sequences. The Back Group is the lowest sequence and is comprised of felsic to intermediate flows, tuffs and breccias. The Hackett River Group overlies the Back and consists of  volcanic flows that range from felsic to mafic, as well as tuffs and chemical sediments. The uppermost sequence is the Beechey Lake Group, comprising turbidite sediments, greywacke, mudstone and iron formation. Recent mapping by the Geological Survey of Canada suggests that the Hackett River and the Back volcanic belts, which are generally spatially separate, may be coeval in their upper parts (Williamson and Olson, 1990).  At least four periods of deformation have affected the Yellowknife Supergroup. Metamorphic grade in the Back River Region ranges from sub-greenschist to upper amphibolite facies.  Three periods of iron formation deposition have been identified within the Back and Beechey Lake Groups (Chandler et al, 1992). In the property area, iron formations are believed to be equivalent stratigraphically to the uppermost iron formations in the Beechey Lake Group.  "
076GNE0017,77,2,"The Beechey Lake Group in the Back River Region are isoclinally folded greywackes, siliceous greywackes and mudstones that are interbedded with iron formation and are steeply dipping. The iron formation consists mainly of magnetite and chert and are of the oxide variety. Subordinate amounts of silicate iron formation are also present (Williamson and Olson, 1990)  Map 5602-70 from assessment report #081975 shows the location of the Goose Lake area.  The Goose Lake showing is within a northwest plunging antiformal closure. Gold zones appear axial planar to the fold structure and reasonably continuous in nature. The mineralization is interpreted to occur in three subparallel zones occupying the west limb, fold nose and east limb of the fold structure. The deposit is completely open down plunge and along the strike of the limbs (Chandler et al,1992). The Goose Lake iron formation has a NNW strike and is at least 8 km long and 1.5 km wide.  The Goose Lake Showing is a NW plunging antiformal structure that is comprised of a sequence of interbedded greywacke, oxide iron formation, sillicate iron formation and mudstone. This sequence has been intruded by felsic and gabbroic dykes. The Goose Lake iron formation is believed to be stratigraphically similar to the George Lake iron formation.  The Goose Lake mineralized zones occur in both the west and east limbs of the antiformal structure as well as in the fold nose. Chandler et al,1992 interprets them to be subparallel to the axial plane of the fold and steeply dipping. Increased quartz veining, silicification, the development of chlorite and sulphide replacement of magnetite characterize the gold bearing zones. Three subparallel but spatially distinct zones of higher grade gold value occur in the west limb (West Zone), fold nose (Main Zone) and east limb (East Zone). "
076GNE0017,78,3,"Gold zones appear axial planar to the fold structure and reasonably continuous in nature. The mineralization is interpretted to occur in three zones subparallel to the axial plane of the fold occupying the west limb (West Zone), fold nose (Main Zone) and east limb (East Zone) of the fold structure. The deposit is completely open down plunge and along the strike of the limbs(Chandler et al,1992). The Goose Lake iron formation has a NNW strike and is at least 8 km long and 1.5 km wide.  Increased quartz veining, silicification, the development of chlorite and sulphide replacement of magnetite characterize the gold bearing zones.   Oxide iron formations host the gold bearing sulphidic zones. The sulphidic zones contain up to 8 volume percent euhedral arsenopyrite and 7 volume percent disseminated and wispy pyrite. Near the sulphidic zones the iron formation is chloritic, foliated and graphitic and cut by quartz veins. Flanking the larger oxide iron formation, thin beds of silicate iron formation are present in greywacke. These contain up to 7 volume percent disseminated and wispy pyrite +/or pyrrhotite which occurs adjacent to quartz veins. This silicate iron formations are at least 10 m long and up to 0.75 m wide.  "
076GNE0017,79,4,"Exploration in the Goose Lake area commenced in 1984 with reconnaissance prospecting. A rock chip sample collected at Goose Lake assayed at 1.30 g/t Au across 2.3 m and a grab sample assayed at 17.11 g/t Au (Johnston et al,1985).  In 1985, an airborne DIGHEM geophysical survey, reconnaissance mapping, prospecting and sampling was done over the area, one assay had a value of 4.40 g/t Au.  Exploration in 1986 consisted of detailed mapping, sampling, and ground geophysical surveys of magnetometer, VLF-EM and HLEM. A till sample survey was also done within the Goose Lake area.  Of 25 rock samples collected gold assays ranged from less than 0.7 to 8.67 g/t Au. Four samples assayed between 3.00 and 8.67 g/t Au, two samples assayed from 0.5 and 3.0 g/t Au. Fifteen samples had an anomalous gold value ranging from 0.15 to 0.34 g/t Au.  In 1987 infill grid surveying, prospecting, ground magnetometer and VLF-EM surveys were carried out to extend and delineate the iron formation.  From 1988 to 1991 no field work was done on the Goose Lake area.  In 1992 till sampling, ground geophysics (magnetic, VLF-EM and gradiometer) and diamond drilling of 19 holes totalling 2,729 m. A total of 869 core samples were taken with numerous assays exceding 20 g/t Au (e.g. 77.86 g/t Au over 1.0 m and 127.44 g/t over 1.25 m).  In 1993 a detailed geophysical survey and a legal survey was completed at the Goose Lake property.  In 1994 21 diamond drill holes were drilled totalling 7473 m. "
076GNE0017,80,5,"A press release from Kit Resources on 25 March 1998 announced that a new resource estimate had been calculated based on a drill program from 1997. Twelve drill holes on the Goose Lake target produced the best grades and widths and the deposit remains open to depth. The indicated resource is 1,896,000 tonnes at 10.53 g/t and 642,00 contained ounces gold. Kit  Resources state  they intend to test for depth extension in the next phase of drilling as well as advance the project to prefeasibility stage as market conditions improve. "
076GNW0003,81,1,"The George Lake area lies within the northeastern portion of the Archean Slave Structural Province. The region is bordered by the Aphebian age Bear Structural Province to the west, and the Rae Structural Province to the east. The principal underlying supracrustal rocks belong to the Archean Yellowknife Supergroup and consist mainly of volcanics and metasediments. Archean intrusive and metamorphic rocks also underlie the region. Early Proterozoic (Aphebian) clastic sedimentary and carbonate sequences of the Goulburn Group unconformably overlie the Archean rocks locally. Intrusive rocks of Hudsonian age and younger diabase dykes crosscut the older lithologies.  The George Lake Area is within the Back River region. The Yellowknife Supergroup in the property area is divided informally into three major sequences.  The Back Group is the lowest sequence and is comprised of felsic to intermediate flows, tuffs and breccias. The Hackett River Group overlies the Back and consists of  volcanic flows that range from felsic to mafic, as well as tuffs and chemical sediments. The uppermost sequence is the Beechey Lake Group, comprising turbidite sediments, greywacke, mudstone and iron formation. Recent mapping by the Geological Survey of Canada suggests that the Hackett River and the Back volcanic belts, which are generally spatially separate, may be coeval in their upper parts (Williamson and Olson, 1990).  At least four periods of deformation have affected the Yellowknife Supergroup. Metamorphic grade in the Back River Region ranges from sub-greenschist to upper amphibolite facies.  Three periods of iron formation deposition have been identified within the Back and Beechey Lake Groups (Chandler et al, 1992). In the property area, iron formations are believed to be equivalent stratigraphically to the uppermost iron formations in the Beechey Lake Group. "
076GNW0003,82,2,"The Beechey Lake Group in the Back River region are isoclinally folded greywackes, siliceous greywackes and mudstones that are interbedded with iron formation and are steeply dipping. The iron formation consists mainly of magnetite and chert and is of the oxide variety. Subordinate amounts of silicate iron formation are also present (Williamson and Olson,1990).  The Beechey Lake Group greywackes have been intruded by sill like bodies of Archean felsite. These sills are generally 1-3 m wide with the exception of one at the NW end of George Lake which is up to 130 m wide and 2.3 km long.   The sedimentary rocks and the iron formations of the Beechey Lake Group as well as the Aphebian Goulburn Group sediments have been cut by numerous NNW trending Helikian gabbroic dykes. Approximately 50% of the Precambrian rocks of the George Lake area are mantled by quaternary glacial material.  The metamorphic grade of the Beechey Lake Group in the George Lake area is lower to middle greenschist.  The George Lake area has been subject to an increasing scale of exploration since 1982. The area has been prospected, mapped, trenched, sampled and drilled as well as having airborne geophysics and detailed ground geophysics done.   In the George Lake area, iron formations within Beechey Lake sedimentary rocks strike northwest. This 16 km long and 2.5 km wide iron formation/sediment sequence has three major oxide iron formation belts identified within it. These belts are: the George Lake belt, the Fold Nose belt and the Lookout Hill belt.  Maps 6601-31 & 32 from assessment report 082117 show the three main belts as well as the main mineral occurrences and their locations. All locations of occurrences are taken from an approximate midpoint and located with reference to the George Lake camp (GLC) which is on the SSW shore of George Lake."
076GNW0003,83,3,"Gold exists in sulphide facies within oxide iron formations in several areas in the George Lake area. Five deposits are highlighted but there are numerous gold occurrences throughout the area. Assays (from 1988) marked with an asterick are cut assays to 34.268 g Au/t.  The George Lake North deposit consists of Locale 1 - Locale 1 North. Locale 1 North-Locale 1(approximately 1.2 km NW of GLC) gold bearing sulphidic zone has a minimum strike length of approximately 960 m, an average vertical extent of approximately 200 m and a true width of 3.7 m for intersections with a gold grade times width product over 10 g*m. One drill hole intersected a zone with a weighted average of 9.02* g/t Au over 10.53 m core length.  Locale 1 North (1.8 km NW of GLC) has two oxide iron formations that are the steeply SW dipping limbs of a syncline. The SW limb is gold bearing and ranges from 5 to 50 m wide. Gold in the oxide iron formation is spatially related to quartz veins and the sulphidic zones have abundant quartz and chlorite, up to 15% pyrrhotite and lesser pyrite and arsenopyrite. Visible gold is present with chlorite and sulphides within and near quartz veining.  The Occurrence Lake deposit (formerly Locale 2, approximately 400 m SW of GLC) has a gold bearing sulphide facies iron formation that ranges from 2.72 to 18.77 m wide and strikes for 110 m. Mudstone and greywacke beds are often intercalated with the iron formation. Visible gold is associated with white vein quartz and arsenopyrite veins which crosscut the iron formation. The best drill core result from 1988 produced a weighted average of 4.9 g/t Au over 13.32 m core length.  "
076GNW0003,84,4,"The Esker Pond deposit (formerly GH): The southwest oxide iron formation (approximately 3 km S of GLC) has a gold bearing sulphidic zone that has a minimum strike length of 240 m which extends to a depth of at least 270 m below surface (average depth of 120 m) and an average true width of approximately 4.9 m for intersections with a grade times width gold value over 10 g*m. The iron formation exists in a tight SE plunging syncline. Two drill holes from 1988 gave weighted averages of 8.33 g/t Au over 13.65 m core length and 17.91* g/t Au across 6.14 m core length. GH South (2.5 km S of GLC)has an oxide iron formation within an isoclinal syncline that contains pyrite, arsenopyrite and visible gold associated with chlorite and quartz veining. The gold bearing sulphidic zone has a strike length of at least 120 m in the NE part of the iron formation. The highest weighted average obtained from the 1988 drilling was 2.83 g Au/t over 15.27 m core length.  The Slave deposit (approximately 1.2 km ESE of GLC) has thick oxide iron formation as well as silicate iron formation, both are folded and faulted. Gold exists in sulphidic zones which are spatially related to quartz carbonate veins and usually contain chlorite. Sulphides include pyrite and arsenopyrite. At Slave Central Fold a drillhole intersected a zone which gave a weighted average of 10.94* g/t Au over 10.14 m core length. At Slave Northern Folds, a weighted average of 2.12 g/t Au over 10.55 m core length was obtained.  The Lone Cow Pond deposit (approximately 3.8 km NW of GLC) has a gold bearing zone within a siliceous iron formation and auriferous chloritic greywacke that is interbedded with mudstone. Within the sulphide facies arsenopyrite is found up to 30% volume and pyrite ranges from 2-20% locally. White quartz veins 1-10 cm are found within the iron formation and the greywackes."
076GNW0003,85,5,"The gold bearing zone has two high grade shoots, the larger one plunges approximately 40 degrees NW with a true average width (for grade times width over 10 g*m) of 3.4 m and a down plunge length of 430 m. The shoot ranges from 60-110 m in length perpendicular to plunge axis. The highest gold weighted average from drilling in 1988 was 16.68* g/t Au over 8.23 m core length.  On March 24 1992  a public presentation to the NWT water board gave an undiluted geological resource estimate for the five deposits of the George Lake area as 3.1 million tonnes at a cut grade of 12.41 g/t gold to a 300 m depth.   In 1996 when the George Lake properties changed owners a news release from Arauco Resources Corporation  (July 2, 1996) stated that the George Lake property has over 100 surface gold showings which assayed at over 10 g Au/t.  A 1998 press release from Kit Resources Ltd. announced new resource estimates based on a 21,000 m drill program conducted in 1997. Resource estimate as follows: Locale 1: 1,228,000 tonnes @ 10.84 g/t, 428,000 contained ounces gold Locale 2: 1,063,000 tonnes @ 11.62 g/t, 397,000 contained ounces gold Lone Cow Pond: 381,000 tonnes @ 10.74 g/t, 132,000 contained ounces gold GH: 228,000 tonnes @ 10.22 g/t, 75,000 contained ounces gold Slave: 176,000 tonnes @ 9.88 g/t, 56,000 contained ounces gold  All of the mineralization is located less than 300 metres below surface so a portion of the resource can be mined by open pit. The resource was based on a cutof grade of 5 grams of gold per tonne. 93-95 percent of the gold would be recovered using carbon in pulp milling techniques.  In July of 1998 an independent resource calculation was released in the NOrthern Miner which expanded the size of the gold deposit. It is now estimated to host 6.5 million tonnes averaging 9.76 g/t Au. The increase is attributable to new inferred resources which total 2.22 million tonnes of 9.9 grams gold. The indicated resources total 4.2 million tonnes grading 9.8 grams gold."
076GSW0001,86,1,"The Musk massive sulphide occurrences are located in the Hackett River greenstone belt of the Slave structural province. They occur near the transition between a dominantly mafic sequence and an overlying, dominantly sedimentary sequence. This stratigraphic position is generally occupied by a carbonate-rich, felsic pyroclastic-tuff sequence which is well-developed.   The immediate area of the Musk showing is underlain by a sequence of volcanic rocks capped by chemical sediment. The deposit footwall comprises a complexely interbedded sequence of rhyolite tuffs, lapilli tuffs and crystal tuffs together with minor agglomerate and thin rhyolitic flows. Massive sulphides occur near the top of a well-foliated, recrystallized rhyolitic tuff and are manifested in a number of small gossans sporadically developed over a 700 metre strike length. Immediately overlying this mineralized unit are massive pillowed basalt flows characterized by carbonate amygdules and discontinuous zones of carbonate-cemented breccia. This unit is overlain by a series of andesitic tuffs and flows which is in turn overlain by a package of interbedded rhyolitic, rhyodacitic and dacitic tuffs and agglomerates, all of which are carbonate-rich. This final sequence is capped by cherty, carbonate-rich tuffites.                      Diamond drilling has intersected two zones of base metal enriched massive sulphides. The upper zone comprises disseminated and poorly bedded to veined sphalerite, galena and chalcopyrite with lesser pyrite and pyrrhotite, in an altered felsic lapilli tuff."
076GSW0001,87,2,"The lower sulphide horizon consists of massive sphalerite and pyrite together with lesser pyrrhotite and galena. Chalcopyrite is most typically found as stringer veins and disseminations in the basal portions of the mineralized zones although it is present in minor amounts throughout. Rough banding can be seen in some areas and a gradation from a Zn-rich top to Cu-rich base is apparent in most drill intersections.  Footwall alteration consisting of chlorite, biotite, talc, sericite, garnet and minor anthophyllite is variably developed below the mineralized horizon, which itself is strongly silicified and is characterized by moderate chlorite, biotite and carbonate alteration.  Work has been done on the Musk showing area since 1974 and includes: an airborne survey which identified a two line anomaly, this was followed up with geological mapping and geophysical surveys including magnetometer, VLF-EM, VLEM which identified sulphide mineralization in outcrop. Another pass of geophysical surveys were done later on which included gravity fluxgate magnetometer, HLEM, VLEM and VLF-EM as well as geological mapping and diamond drilling (13 ddh totalling 1395 m). A conductor was identified and drilling intersected high grade massive sulphides. A follow up program of diamond drilling was done (23 ddh totalling 2570 m) which outlined a geological inventory of 387,000 tons grading 1.2% Cu, 1.39% Pb, 10.38% Zn, 10.87 oz/ton Ag and 0.049 oz/ton Au. Note: this geological inventory is based on a total of 36  diamond drill holes.  The latest (1994) work done on the showing was a DeepEM survey. AR 083324"
076LNE0023,88,1,"The showing is in the predominantly volcanic, north-trending High Lake supracrustal belt, which in this area is a mixed succession of Archean Yellowknife Supergroup metavolcanics and metasediments metamorphosed to lower amphibolite facies, and flanked east and west by late Archean plutons. A structural history involving isoclinal folding, at least 3 generations of fabric formation, and late faulting, is not yet unravelled.                      The geology below is largely derived from Flood (1991).                      The Ulu area is a lobe of supracrustal rocks on the west margin of the High Lake belt. It is separated from the main part of the belt by a narrow granitic apophysis. The supracrustals comprise a sequence of basalts, greywackes and gabbroic sills, all folded into a 5 km-long, doubly-plunging? anticline. Later Archean feldspar-porphyry and quartz- diorite dykes and Proterozoic diabase dykes transect this sequence.                      Auriferous zones are near the axis of the north-trending anticline. The largest zone, the Flood Zone, strikes NW and dips steeply for 400 m on the west limb of the anticline, near the sediment-filled core. The main part of the zone is 2 - 5 m thick, increasing to 10 m at points of flexure along the roughly tabular body, and has been intersected at depths over 600 m. Lesser developed, en echelon hangingwall and footwall zones have also been recognized as part of the Flood Zone. Structural features of note include brecciation and re-brecciation, vein paragneiss, and local mineral segregation in shear banding. These point to multiphase brittle and ductile deformation.                      Auriferous zones comprise intense silicification and acicular arsenopyrite development to 5%; arsenopyrite occurs as needle aggregates within veins and fractures and as complete replacement of basalt breccia fragments."
076LNE0023,89,2,"Gold occurs mainly at quartz-arsenopyrite boundaries. Pyrrhotite, pyrite and minor chalcopyrite are present as well as a variety of alteration minerals (see Mineralization section). An alteration envelope comprising a stockwork of quartz-actinolite veins and biotite-microcline enrichment extends 2 - 5 m from the ore zone. This is consistent with the K-enrichment and Na-depletion characteristic of Archean hydrothermal systems.                      Quartz-actinolite veins within the Flood Zone strike more northerly than the zone itself, which is approximately perpendicular to the regional foliation (S3), suggesting a left-stepping en echelon array (Henderson 1993).                      Reserves are guesstimated by DIAND geologists at over 1 million tonnes of greater than 10 g/t Au."
076LSW0008,90,1,"The Gumbo Lake Ilmenite deposit is hosted by a late Archean or early Proterozoic mafic complex, intrusive into Archean Yellowknife Supergroup metavolcanics of the Kathawachaga (Southern) segment of the High Lake supracrustal belt. This segment trends NE and is cut off from the High Lake belt proper by, and surrounded by, batholithic intrusions of late Archean granitoids. It has undergone polyphase Archean deformation, and metamorphism to greenschist facies.                      The host mafic complex intruded NE to north striking, moderately to steeply west dipping massive basalts and tuffaceous dacites at the extreme northeast end of the Kathawachaga segment. The gabbro-norite and leuconorite complex is elongated NNE and shallowly dipping.                      A roughly circular, more mafic component of the complex, near its centre, comprises noritic metagabbro. This varies from meso to leucocratic, and from diabasic to porphyritic and cumulate-textured. Ilmenite in this central mafic part of the complex is ubiquitous as an accessory, and in two significant pods varies from 10% to 70% of the rock. The Eastern and Western pods, 400 m apart, were gridded and sampled at 7.6 m intervals, but roughly half the 105 samples were destroyed by fire before assaying, leaving 34 from the Eastern grid and only 8 from the Western. From these a rough approximation of tonnage was arrived at for the Eastern zone (AR 080184), with grades somehow higher than any of the component sample assays: 252,000 square ft (61,550 tons/vertical ft) at 18.42% Fe, 0.22% V and 11.86% Ti. The surface expression of the pod is approximately 600 m long in a northerly direction and 100 m across, though ""the limits of the ilmenite are not defined precisely on both grids"". The Western pod is approximately 500 m NNE by 140 m, cut by an ENE fault at its north end."
076LSW0008,91,2,"Its grade is estimated to be at least equal to that of the Eastern pod; 3 samples along 15.2 m averaged 15.50% Fe, 0.16% V and 9.60% Ti.                      Numerous granitic dykes intrude the complex.                      Roscoe (GSC Paper 1985-1A) suggests the complex is part of the Booth River Intrusive Suite, a layered mafic/ultramafic complex 60 km to the east, intruded after Archean granitoids and before Aphebian Goulburn Group sediments."
076MNW0084,92,1,"The Anialik River Intrusive Complex hosts the North Vein, which includes the North Central Vein deposit at its northeast end and the North Vein South Zone showing at its southwest end, as well as numerous other auriferous, shear-hosted quartz veins collectively known as the Arcadia or Coronation Gulf showings. Relief in the area is approximately 60 m, exposure about 50%.  The complex is an elliptical, NNE-trending, 35 by 15 km pluton whose gold showings are concentrated in the northwest portion. Its dominant phase is a variably deformed and altered leucotonalite with subordinate trondhjemite. Locally intermixed mesotonalite forms a variety of migmatitic textures. Such rocks host most of the North Vein system, including North Central Vein. Mafic phases and intensity of deformation in the pluton increase toward its margins, so that a margin-parallel band of mesotonalite hosts the southwest end of the North Vein system, and grades west into the mafic marginal phase (Abraham 1989), a heterogeneously deformed band of foliated, sheared or migmatitic diorite, mesotonalite, and gabbro. The actual contact of the pluton with supracrustals, approximately 1km west of North Central Vein, is the sheeted zone of Abraham, a 200 - 800 m wide shear zone comprising mylonitized equivalents of: plutonic rocks; metavolcanics; and numerous, foliation-parallel, ""sheeted"" felsic dykes.  The complex is covered on the north by water. It is surrounded on all other sides by predominantly felsic metavolcanics of the Anialik River volcanic-(sedimentary) belt, and is thought by Abraham (1990, 1991) to be largely coeval with them and emplaced diapirically into them. Tonalites from the complex gave zircon ages ranging from 2703 +/- 2Ma in the mafic marginal phase, to 2694Ma in the North Central Vein hanging wall, progressively younger eastward to 2682Ma."
076MNW0084,93,2,"Recent dates from the volcanic belt give roughly the same span of activity yielded by the tonalites, minus the oldest date (Villeneuve 1992 dates referred to by C.Relf, Geoscience Forum, DIAND Yellowknife 1992).  The pluton is cut by at least five generations of dykes: sheared, boudinaged and chloritized gabbro dykes; later (syn-intrusion?) intermediate dykes; and three sets of felsic dykes distinguished by orientation. Two of the felsic sets are sheared, boudinaged, folded and locally mylonitized, and may have been loci for development of shear zones; they are locally mineralized where they occur in auriferous shears (eg. North Central Vein). The third set of felsic dykes commonly cross-cuts the other two but locally is cross-cut by them, and never cross-cuts mineralized shears. All are regarded as pre to syn-shearing.  Syn to post-tectonic granitoid plutons intrude the complex and the surrounding volcanics 6 km southwest and 2 km northwest of the deposit. Late Proterozoic diabase dykes trend northwest throughout the area, and Proterozoic gabbro sills cap the Archean rocks approximately 3.5 km north of the deposit.  The pluton records two phases of Archean deformation (Abraham 1989, 1990, 1991) although three are recognized in the surrounding supracrustals (Relf 1992). D1 apparently coincided with diapir emplacement and generated a margin-parallel foliation throughout the complex and some isoclinal folding in the western portion. Metamorphism of the surrounding volcanics to amphibolite grade and development in them of a margin-parallel S1, also took place at this time.  "
076MNW0084,94,3,"D2 is thought by Abraham to have been a regional translational shearing event. It produced a mild to intense, northerly to northeasterly fabric in the complex, as well as discrete zones of mylonitization including four major shears and dozens of minor ones. All the mineralized shears are thought to be D2. Most of them strike NE but some strike NNW.  The last deformation was Proterozoic east to west, dextral and sinistral faulting which offset Archean fabrics and late diabase dykes.  North Central Vein belongs to the North Vein system, which is exposed intermittently in anastomosing shears for 5.5 km. The North Central Vein is thought to have developed by fracture-controlled, multiple-stage quartz injections. It consists of quartz stringers, pods and lenses, and locally of quartz matrix to a breccia of mylonitic wall-rock fragments. The North Central Vein strikes northeast for 700 m and is approximately 1.5 m wide. Gold mineralization is found within the quartz, and within cross-cutting, mylonitized felsic dykes. Quartz was apparently injected in three stages, the first two late in the D2 event (Abraham). Gold has so far been identified in the first stage only, associated with highly deformed pyrite. The second stage relates to extensive hydrofracturing and euhedral pyrite. The third consists of post-tectonic quartz-(carbonate) in-filling and often contains specular hematite.  The age of the syn-shearing mineralization is bounded by the youngest tonalite age (2682 +/- 2Ma) and the age of the post-tectonic Chin Lake Stock, 6 km SW of the deposit (2602 +/- 2Ma). A hydrothermal alteration event at 2670Ma is recorded in titanite from the North Central Vein hanging wall; this may be related to the mineralizing event (Abraham 1990)."
076MNW0084,95,4,"Excitement over the North Central Vein was generated in the 1960s when 320 feet at its south end was opened by 10 trenches averaging 0.84 oz/ton Au across 5 ft, four trenches along 160 ft in the middle averaged 0.48 oz/ton across 4 ft, and 26 trenches along 1200 ft at the north end averaged 0.33 oz/ton across 5 ft. By 1987, the Vein had been tested by 74 trenches, over 150 drill holes and three bulk samples. Reserves of 160,772 tons of 0.353 oz/ton Au proven, probable and possible, and of 737,000 tons of 0.205 oz/ton Au proven and probable, have been outlined using different methods with the same data (see Reserves section of this report).  The No.11 Vein of 1965 is just northeast of the 1965 North Vein, perhaps part of the same system. It returned trench sample assays averaging 13.03 g/t Au across 1.4 m and 60 g/t across 0.9 m. Its relationship to the current North Central Vein is uncertain; it is definitely nearby and may be regarded as part of it."
076MNW0085,96,1,"The Anialik River Intrusive Complex hosts the Fred Vein deposit and numerous other auriferous, shear-hosted quartz veins collectively known as the Arcadia or Coronation Gulf showings. Relief in the area is approximately 60 m, exposure about 50%.  The complex is an elliptical, NNE-trending, 35 by 15 km pluton whose gold showings are concentrated in the northwest portion. Its dominant phase is a foliated to gneissic leucotonalite with subordinate trondhjemite. Locally intermixed mesotonalite forms a variety of migmatitic textures. Such rocks host the Fred Vein. Mafic phases and intensity of deformation in the pluton increase toward its margins, through a margin-parallel band of mesotonalite to a heterogeneously deformed band of foliated, sheared or migmatitic diorite, mesotonalite, and gabbro (the mafic marginal phase of Abraham 1989). The actual contact of the pluton with supracrustals, approximately 1.5 to 2 km west of Fred, is the sheeted zone of Abraham, a 200 to 800 m wide shear zone comprising mylonitized equivalents of plutonic rocks, metavolcanics, and foliation-parallel felsic dykes.  The complex is covered in the north by water. It is surrounded on all other sides by predominantly felsic metavolcanics of the Anialik River volcano-(sedimentary) belt, and is thought by Abraham (1990, 1991) to be largely coeval with them and emplaced diapirically into them. (For age dating, see the North Central Vein entry in this database.) It is cut by a set of altered mafic dykes, another of intermediate dykes, and three sets of felsic dykes. All are pre to syn-shearing."
076MNW0085,97,2,"Syn to post-tectonic granitoid plutons intrude the complex, and the surrounding volcanics, 8 km southwest and 3 km northwest of the deposit. Late Proterozoic diabase dykes trend northwest, and Proterozoic gabbro sills cap the Archean rocks approximately 3.5 km north of the deposit.  The pluton records two phases of Archean deformation (Abraham 1989, 1990, 1991) and one of Proterozoic faulting (for more detail see North Central Vein). All the mineralized shears are thought to be D2. Most of them strike NE but some strike NNW. Quartz injection and gold mineralization took place late in D2.  The Fred Vein is roughly 250 m long. Its relationship to the Pick and Northwest Veins of 1965 is uncertain but it is probably nearby. Pick was opened in 13 trenches which ran from 2.74 g/t Au across 0.3 m to 30.86 g/t across 1.22 m. Northwest Vein yielded a grab of 78.17 g/t and a best chip of 26.06 g/t across 0.5 m. In the Fred Vein, reserves of 38,338 tons of 0.44 oz/ton Au proven, probable and possible, and of 101,000 tons of 0.25 oz/ton Au proven and probable, have been outlined using different methods with the same data (see Reserves section of this report)."
076MSE0053,98,1,"The High Lake AB Zone is within the north-trending High Lake supracrustal belt, which comprises mainly Archean Yellowknife Supergroup metavolcanics.  The High Lake deposits are hosted by a 200 m wide unit of altered and sheared, felsic and intermediate pyroclastics, consisting of fragments of dacite and siliceous rhyolite in an andesitic to dacitic matrix.  A rhyolitic flow and narrow bands or lenses of carbonate-cemented, felsic breccia are interbedded with the pyroclastics of this unit, east of the deposits. This unit is part of a north-striking, steeply dipping succession, and is underlain to the east by massive, pillowed and tuffaceous andesites and dacites, and overlain to the northwest by rhyolite or rhyodacite tuffs.  The AB Zone, approximately 600 m north of the D Zone (separate report in this database), is a series of subconformable, Cu-rich, stringer-dominated sulphide lenses, striking northeast and plunging north, within intensely altered rocks (see Mineralogy). The zone measures maybe 150 by 75 by 75 m; it is exposed on surface as two discontinuous, NE-trending gossans, ""A"" 300 m long and ""B"" 150 m long, with a combined width of approximately 75 m. Zn content increases westward, toward the stratigraphic top of the deposit. The AB Zone has potential reserves of 2.9 million tonnes grading 5.75% Cu, 1% Zn, and 1.02 g/t Au (AR 061730, 1974; also quoted in Northern Miner Nov 4/91).  Less than 75 m west of AB Zone is a major mixed intrusion comprising mainly amphibolite and gabbro with numerous volcanic inclusions; however, near the orebody its composition is granodioritic to dioritic. It is elongate parallel to stratigraphy for a number of kilometres, and is thought to be syn-kinematic and responsible for contact metamorphic effects in the volcanics."
076MSE0053,99,2,"These range from hornblende-hornfels metamorphism and recrystallization, to the development of dalmatianite in the already-altered ore host (see Mineralogy).  A younger, late Archean, granitic batholith is exposed approximately 3km east of the deposit.  Deformational history involving at least two phases of Archean folding is obscured by intense northerly shearing and common northwesterly faulting. The AB Zone itself is sheared and cut by faults. A 1 m wide, late Proterozoic diabase dyke cuts north through the deposit area, and a 10 m wide one follows a NW-trending fault through both the AB and D Zones, offsetting the latter by about 40 m dextrally. The Kennarctic River, 1 km east of the deposit, traces a regional, north-trending shear zone."
076MSE0054,100,1,"The High Lake D Zone is within the north-trending High Lake supracrustal belt, which comprises mainly Archean Yellowknife Supergroup metavolcanics.  The High Lake deposits are hosted by a 200 m wide unit of altered and sheared, felsic and intermediate pyroclastics, consisting of fragments of dacite and siliceous rhyolite in an andesitic to dacitic matrix.  A rhyolitic flow and narrow bands or lenses of carbonate-cemented, felsic breccia are interbedded with the pyroclastics of this unit, east of the deposits. This unit is part of a north-striking, steeply dipping succession, and is underlain to the east by massive, pillowed and tuffaceous andesites and dacites, and overlain to the northwest by rhyolite or rhyodacite tuffs.  The D Zone polymetallic deposit, approximately 600 m south of the AB deposit, is a NE-striking, W-dipping, 100 m long by 100 m deep zone, ranging from 18 m thick near surface to 60 m at depth. It comprises mainly finely disseminated, and locally stringer and banded, sulphides within intensely altered rocks (see Mineralogy). The E zone, 180 m east of D Zone, and the C zone, approximately 300 m north of D Zone, are included here with the D Zone. They have generally ""low"" base metal values, while the D Zone has potential reserves of 4.1 million tonnes grading 2.51% Cu, 4.20% Zn, and 29.5 g/t Ag (AR 061730, 1974; also quoted in Northern Miner Nov4/91).  About 125 m west of D Zone is a major mixed intrusion comprising mainly amphibolite and gabbro with numerous volcanic inclusions; however, near the orebody its composition is granodioritic to dioritic. It is elongate parallel to stratigraphy for a number of kilometres, and is thought to be syn-kinematic and responsible for contact metamorphic effects in the volcanics."
076MSE0054,101,2,"These range from hornblende-hornfels metamorphism and recrystallization to the development of dalmatianite in the already-altered ore host (see Mineralogy).  A younger, late Archean, granitic batholith is exposed approximately 3 km east of the deposit.  Deformational history involving at least two phases of Archean folding is obscured by intense northerly shearing and common northwesterly faulting. The D Zone itself is sheared and faulted. A 1 m wide, late Proterozoic diabase dyke cuts north through the deposit area, and a 10 m wide one follows a NW-trending fault through both the AB and D Zones, offsetting the latter by about 40 m dextrally. The Kennarctic River, 1 km east of the deposit, traces a regional, north-trending shear zone."
076NSE0006,102,1,"The Pistol Lake iron formation-hosted gold deposit is located in a supracrustal basin in the northern part of the Slave structural province. All stratified rocks have been metamorphosed to lower amphibolite facies. Significant gold mineralization is present in two iron formations (IFs) situated within a tightly folded and overturned sequence of medium grade turbiditic sediments dipping west at about 40 degrees. Host turbidites are distal in character, exhibiting A(D)E divisions of the Bouma sequence. The older iron formation is silicate facies and hosts the F and Farney auriferous zones while the younger is oxide facies and hosts the G Zone. The iron formations are separated by about 225 metres of metasediment. No metavolcanic rocks are present in the immediate area. A late granitoid intrusive cuts the sequence about 2 km north of the gold occurrences. The silicate iron formation is up to 10 metres thick and is banded on a number of scales, from mm sized laminae of amphibole, chert and biotite-garnet schist to decimetre scale intercalations of iron formation with clastic sediments. Significant levels of gold occur in highly siliceous iron formation where it is deformed into 50 - 150 metre scale folds. Away from these folds, the iron formation decreases both in thickness, silica content and the number of included amphibolitic bands. Sulphide minerals include pyrrhotite and arsenopyrite, the latter commonly containing cores of loellingite. Pyrrhotite occurs most commonly in fine grained laminae while arsenopyrite usually forms larger subhedral to euhedral crystals, often scattered along pyrrhotitic laminae and in aggregates in the vicinity of cross-cutting quartz veins. Gold occurs as 5 - 100 micron grains in arsenopyrite, frequently at the boundary between that mineral and its loellingite core."
076NSE0006,103,2,"The oxide iron formation is composite in that it consists of a series of stacked facies types with an aggregate thickness on the order of 50 metres. A basal horizon of silicate IF is successively overlain by finely laminated oxide IF, silicate IF, graphitic chert and a series of decimetre scale intercalated amphibolite and clastic metasedimentary beds. Significant levels of gold occur in the G Zone, situated at the base of the laminated oxide IF unit where stratabound arsenopyrite-pyrrhotite mineralization is associated with irregular quartz veins and masses along with recrystallized silicate minerals. Recrystallized areas commonly exhibit disrupted and brecciated textures, with variably mineralized fragments in a matrix of silicate and sulphide minerals. Two main types of sulphide distribution exist. The most important in terms of gold content is characterized by ragged blebs and coarse disseminations of pyrrhotite occurring in recrystallized areas proximal to quartz veins. Arsenopyrite is almost always present and occurs as subhedral crystals and crystal aggregates. It often contains inclusions of pyrrhotite and cores of loellingite. Gold is found as grains up to 100 microns across in arsenopyrite, often at the boundary with loellingite, and as larger grains up to 2 mm across in the silicate matrix. Visible gold is commonly observed in drill core. The second type of mineralization preserves the morphology of laminated oxide IF except that magnetite is replaced to a variable extent by pyrrhotite. Where replacement is extensive, crystals of arsenopyrite are scattered along pyrrhotite-rich bands. Gold is present in the former as grains up to 10 microns across."
076NSE0006,104,3,"Numerous trenches were opened and sampled, and a total of about 11,080 metres in 66 diamond drill holes were drilled, mainly in the F, G and Farney zones (Farney is covered in a separate report), between 1964 and 1988. A small amount of this information is published in Assessment Reports, including such F Zone intersections as 34 g/t Au over 3.0 m and 36 g/t over 1.5 m in hole PL-1, and 7.9 g/t over 1.5 m, 12.5 g/t over 3.0 m and 3.8 g/t over 1.5 m in PL-2, and trench samples of 18.5 g/t Au across 0.9 m from F Zone and 27.4 g/t across 0.6 m in G Zone. Most of the results, however, are not public. Reserves in the northern part of F Zone were estimated in 1984 at 218,337 indicated tonnes averaging 14.78 g/t Au, and reserves in F and G Zones combined were estimated in 1985 at 489,880 tonnes at 13.92 g/t Au (Silver Hart Mines Letter to Shareholders)."
076NSE0010,105,1,"The Turner Lake area lies in the NE corner of the Slave Province, just west of Bathurst Inlet, toward the north end of the Hood River Sedimentary Belt. This belt is a roughly H-shaped, NE-trending area underlain by Archean Yellowknife Supergroup clastic sediments and minor volcanics, locally intruded by pre-metamorphic amphibolitic bodies. It has been affected by at least two phases of Archean deformation, metamorphosed up to middle amphibolite facies, and is flanked and locally invaded by late Archean granitic rocks. It is cut off at its NE end by the Bathurst Fault, which has juxtaposed Aphebian Goulburn Group sediments, to the east, against the Archean rocks, to the west. Late Proterozoic gabbro sills and diabase dykes intrude all other lithologies.  The Turner Lake area is characterized by 30 - 130 m relief and approximately 60% outcrop, ranging from extensive in uplands to none in valleys (AR 082608). The deposit itself is poorly exposed. It lies about 800 m west of Turner Lake, in an area underlain mainly by turbiditic greywackes and minor argillites in a steeply dipping, E-facing, N-striking homoclinal succession. Interbedded with or conformably intruding the sediments are beds of polymict, clast-supported conglomerate, metadiorite synvolcanic? sills, banded amphibolitic rocks, and the host mineralized amphibole-plagioclase schist, all belonging to the Yellowknife Supergroup, and sheets of granodiorite of later Archean age. Pods of pegmatite cross-cutting these lithologies are probably related to the undeformed, late Archean granitic batholith exposed 2.5 km west of the deposit. A plug of undeformed but metamorphosed, Proterozoic? (Schaan 1992) olivine gabbro intrudes the sediments 2.4 km south of the deposit and hosts significant Ni mineralization (the Nickel Knob showing)."
076NSE0010,106,2,"NW-trending diabase and gabbro dykes and sills of at least 2 Proterozoic generations are exposed near the deposit as well.                      The high degree of deformation and alteration within the older Archean rocks has hampered determination of protoliths. A N to NNE-striking, braided shear zone transects the region, leaving rocks within and to either side of it with a pronounced shear fabric. 300 m to 1000 m scale drag folds are well developed on the east side of the shear. The Turner Lake Main Gold deposit lies in the nose and on the north limb of one such 300 m wide, E-closing fold.                      The fold is defined primarily by a banded (feldspar?) chlorite? biotite-amphibole schist or gneiss, perhaps an altered mafic or ultramafic intrusive or mafic extrusive (see Comments under Host Lithology). The structure plunges almost vertically, closing to the east about a steeply dipping, E-W axial plane. The north and south limbs form an angle of approximately 60 degrees and dip steeply south and north, respectively. Metadiorite lies in the core of the fold, and metasediments surround it, along with a metadiorite ""sill"" in the sediments off the north limb. Granitic pegmatites intrude the sediments and amphibolitic schist of the south limb. The west end of the fold merges with strongly sheared metadiorites and mafic and felsic rocks in the regional shear zone.                      Within the banded, amphibolitic schist are a number of sill-like bodies comprised of plagioclase, amphibole, biotite (see Comments under Host Lithology). The largest of these is the primary host and is cut by a quartz stockwork of subparallel, centimetre-scale veinlets forming oblique to perpendicular angles with the margins of the unit, and locally extending into the secondary host (banded amphibolitic schist)."
076NSE0010,107,3,"Gold is associated with sulphides, which are associated with quartz veining. The principal sulphides are pyrrhotite, which is disseminated throughout the quartz-veined rock, and arsenopyrite, which is concentrated in and around the quartz veins themselves. The quartz veins are of more than one generation, and some are marked by hornblende - cordierite - sillimanite? garnet selvages which may be hydrothermal alteration assemblages further altered by regional metamorphism (Clode 1987). The best gold tenors are in the nose of the fold and in the noseward portion of the north limb.  A regional foliation strikes NE and dips steeply NW (AR 082608). Movement on the major N to NNE shear was sinistral, and localized E-W folds with associated axial planar foliations, such as hosts the Main Gold deposit, may have formed as drag folds during the shearing event (AR 082608, Clode 1987, Schaan 1990).  Metamorphic grade is middle amphibolite, except within the shear zone where upper amphibolite conditions and incipient melting have produced a sillimanite - cordierite - microcline gneiss from a granodioritic or pelitic protolith (Clode, 1987, AR 082608).  Based on earlier subdivisions (eg. AR 017152), the deposit is here described in 3 zones and a fourth sample location: the easternmost Nose zone (weighted average chip samples including 8.42 g/t Au across 13.7 m), NC (north-central) zone approximately 250 m WNW of Nose (chips including 11.17 g/t across 5.4 m), NW (northwest) zone approximately 400 m WNW of Nose (chips including 17.76 g/t Au across 1.8 m), and W (west) location approximately 600 m WNW of Nose, which yielded anomalous grabs (5 and 18 g/t) apparently from float transported from the other zones."
076NSE0010,108,4,"Reported DDH intersections tend to be lower grade, except some recent holes (Silver Hart Annual Report 1987) which cut such intersections as 8.9m grading 12.86 g/t. A 1987 reserve estimate based on 17 widely-spaced DDH and chip and panel chip samples from 47 trenches, mostly in and near the Nose zone, is 1.18 million tonnes grading 5.35 g/t Au."
076ONE0010,109,1,"Boston is a gold-bearing shear zone located in the southern portion of the Hope Bay Greenstone Belt.  The Belt is composed of volcanic and sedimentary rocks of Archean aged.  The shear has a strike length of approximately 70 kilometres.    The mineralized shear was first dicovered in 1988 by Abermin Corporation who outlined 9 kilometres of intense quartz-carbonate shearing.  Government geologists from RWED and DIAND provided follow up mapping of the area.  The Boston claims were staked in 1991 by BHP Minerals Canada Ltd. and exploration on the property commensed sortly afterwards.  By 1997 an underground ramp was developed into the shear zone and over 50,700 metres of coring was completed.  A resource calculation was also preformed on Boston resulting in figures of  2 to 3 million ounces of gold (reference RWED RWED, MOG Book (1997))."
085BNE0001,110,1,"The various mineralized zones comprising the Great Slave Reef Mississippi Valley type Pb-Zn deposits are located in the Pine Point Pb-Zn district immediately south of Great Slave Lake. Mineralization occurs in a large, middle Devonian barrier reef complex separating two depositional basins in the Interior Platform, the northern Mackenzie shale-carbonate basin and the southern Elk Point evaporite-carbonate basin. The reef complex consists of a lower Pine Point Formation buildup of skeletal-derived carbonate sands and muds, and an upper Sulphur Point Formation buildup of biohermal to bioclastic limestone.  Most of the Pine Point district Pb-Zn mineralization was deposited in interconnected paleokarst networks that developed at the lower limits of coarse dolomite alteration (known as Presquile dolomite) within the Sulphur Point limestones. The karst networks are present in two main zones known as the North and Main trends. Sphalerite, galena, pyrite and marcasite occur as replacements and open-space fillings within karst openings and in vuggy wall-rock peripheral to the karst openings.  The Great Slave Reef deposits are situated immediately west of the Pine Point property at depths between 150 and 300 m. Grid drilling resulted in the discovery of four deposits. Two more were discovered through followup work on IP anomalies and one deposit was found on the basis of geological and trace element data. By the end of 1981, a total of seven deposits containing an aggregate tonnage of 7.25 million tonnes grading 10.3% combined Pb and Zn had been outlined."
085INE0023,111,1,"The XL base metal massive sulphide prospect is located in the Turnback Lake area. It lies in the Beaulieu Volcanic Belt, a supracrustal belt in the Archean Slave structural province. Volcanism in this portion of the greenstone belt commenced with the eruption of the tholeiitic Tumpline Basalt and concluded with an approximately equal volume of felsic volcanics referred to as the Turnback Rhyolite. Metaturbidites of the Burwash Formation overlie the Turnback Rhyolite. A carbonate exhalite unit is commonly developed at the contact between them. Volcanics and sediments, all part of the Yellowknife Supergroup, are metamorphosed to amphibolite facies. Stratified rocks are strongly deformed around the Sleepy Dragon Complex.  The XL prospect was discovered in 1937 by prospectors Lars Johnson and Garfield Smith, and was optioned by Westfield Mining Company Ltd. in 1938. Westfield drilled 14 holes totalling 2450 ft, excavated 15 trenches, completed geological mapping at a scale of 1:480 and conducted a dip needle survey. No direct record of this work exists and the desciption below, as well as the description of mineralization, is taken from summaries by W.M. Little in AR 017321 and C.S. Lord in GSC Memoir 261.  Mineralization tends to occur within the Burwash Formation along or near the contact between it and the Turnback Rhyolite, in places within the carbonate exhalite between them. It has been divided into four zones, the A, B, C and N. These appear to lie within a 40 m thick stratigraphic interval over a total strike of about 600 m but are separated by intervals of relatively weak mineralization. In parts of the 40 m interval, only one sulphidic band is present, while in other parts, four or more occur over the 40 m."
085INE0023,112,2,"Massive and disseminated pyrrhotite, sphalerite, chalcopyrite, galena and pyrite are present (in that order of abundance). The N zone occurs in amphibolite and differs somewhat in that it consists of a large number of discontinuous stringers and fine disseminations of chalcopyrite, along with about 1% pyrrhotite as fine disseminations. Very minor sphalerite and a few specks of native copper are also present. AR 082901 notes the abundant development of a needle-like amphibole in the vicinity of the XL deposit and the OK deposit to the southwest. This is tentatively interpreted as the metamorphic derivative of hydrothermal alteration in the enclosing rocks.  AR 017321 estimates a reserve of 910 tons per vertical foot at a grade of 6% Zn, 2% Cu, 1.5% Pb and 3 oz/ton Ag. Apparently, drilling by Westfield suggested that mineralization was cut off by granite at a depth of about 200 feet at the A zone and would probably be truncated above a 500 foot depth elsewhere. AR 082654 restates the reserve figure as an aggregate reserve of 180,000 tons at the same grades and to a depth of 90 m."
085INE0086,113,1,"The Sunrise volcanogenic massive sulphide deposit occurs in the Beaulieu River supracrustal belt, a predominantly volcanic belt in the Archean Slave structural province. All stratified rocks in the belt belong to the Yellowknife Supergroup, the volcanics in the Sunset Lake area belonging to the Beaulieu Group. The stratigraphic sequence forming the footwall of the deposit begins with a rhyolitic lapilli tuff to agglomerate known as the Western Rhyolite, and continues upward with tuffaceous argillite, sericitic felsic tuff and rhyolitic pyroclastic breccia. Sulphide mineralization occurs at the contact of the pyroclastic breccia with an overlying, sericitized and occasionally chloritized, fine grained felsic tuff. Immediately overlying these mineralized and altered units is a mafic package including intermediate to mafic pillowed flows and lapilli tuffs. This is in turn overlain by a felsic package including sericitized quartz eye rhyolitic tuff, argillite, intermediate flows and felsic fragmentals, and then by a thick package of intermediate to mafic flows. The sequence generally strikes northnorthwesterly and dips to the east at 65 - 80 degrees. A sinistral NE fault, named the Campsite Fault, has offset stratigraphy by about 1400 metres. The Bear massive sulphide deposit owned by Silver Hart Mines Ltd. across the fault appears to be at the same stratigraphic level as the Sunrise deposit.                      Sulphide mineralization includes pyrite, sphalerite and galena with lesser tetrahedrite, arsenopyrite, pyrrhotite and chalcopyrite. Other metallic minerals identified to date include pyrargyrite, boulangerite, native silver, native gold, gudmundite and stannite. The base of the sulphidic sequence is constituted by a layer of semi-massive sulphides which is actually a strongly brecciated rhyolite with a sulphide matrix."
085INE0086,114,2,"The main sulphide lens includes very well banded, fine to medium grained material together with massive, coarse grained sulphides, the latter being brecciated in places. Coarse lithic fragments within the sulphide horizon suggests proximity to a vent.                      Footwall stringer mineralization is described only as minor stringers of sphalerite and galena, patchy pyrite and minor chalcopyrite accompanied by silicification. The discovery outcrop consists of this stringer style mineralization and a sample returned a value of 35 g Au/tonne. A limited lithogeochemical study suggests strong Na2O depletion.  The deposit has been outlined by 65 diamond drill holes which show a strike extent of 160 metres and an average thickness of 3 - 4 metres. It has been traced down dip for 700 metres and is open to depth. A steep northerly plunge of about 65 degrees is evident in longitudinal section. Reserves are estimated at over two million tonnes grading 8.88% Zn, 4.22% Pb, and 400 g/t Ag (Aber Interim Rpt, 10/31/88)."
085INE0087,115,1,"The Bear or M-zone volcanogenic massive sulphide deposit occurs in the Beaulieu River greenstone belt, a supracrustal belt in the Archean Slave structural province. All stratified rocks belong to the Yellowknife Supergroup, the volcanics in the Sunset Lake area belonging to the Beaulieu Group. Stratified rocks are intruded by late Archean gabbro and granite as well as Proterozoic diabase dykes. Massive sulphides are hosted by an east facing, northwesterly trending and easterly dipping sequence of volcanic and sedimentary rocks.  The base of the sequence in the immediate vicinity of the deposit is constituted by a series of pillowed to massive andesites to basalts. Thin units of fragmentals and interflow sediments are present in places within this unit. Several kilometres to the north and to the west, this unit includes oxide iron formation. Overlying the mafic package is a unit of quartz feldspar porphyritic rhyolite flows and fragmentals, part of which appears to form a small endogenous dome. Alteration in the form of kaolinitization, sericitization and silicification is present. The rhyolites are in turn overlain by a sequence of mixed greywacke, chert, graphitic argillite and mafic to felsic tuff. M zone massive sulphides occur as two separate horizons at this point, a lower silver-rich, narrow (2 m) zone sandwiched between a graphitic argillite beneath and a carbonate-rich exhalite above, and a thicker (15 m) zone in an overlying unit of rhyolitic tuff to coarse pyroclastics. The mineralized horizons are successively overlain by pillowed to fragmental mafic volcanics, intermediate fragmentals and flows, and then argillite. A thick quartz feldspar porphyry sill occupies the contact between the mafic and intermediate units."
085INE0087,116,2,"The lower mineralized zone is generally less than 2 metres thick and consists of a base of laminated pyritic argillite grading upward into semi-massive pyrite with minor base metals and then into variably bedded massive sphalerite, galena, pyrite and sternbergite. A thin (20 cm), greenish and pasty band of sphalerite, sternbergite, marcasite, galena and other silver minerals overlies the massive sulphides. This lower zone is separated from the upper mineralized zone by a unit of felsic fragments, carbonate, minor argillaceous material and variable amounts of sulphides together with tuffaceous greywacke.  The upper mineralized zone consists of a base of semi-massive to massive pyrite successively overlain by massive pyrite with variable but minor base metal sulphides, and semi-massive to banded sphalerite and galena with only limited amounts of pyrite. A third and minor sulphide horizon with a sulphidic argillite base is seperated from the upper mineralized zone by a debris flow.  Drilling has traced the M zone horizons over a strike length of 160 metres and to a depth of about 400 metres. Longitudinal sections show a north northeasterly plunge of about 70 degrees for the deposit, which is open to depth."
085INE0149,117,1,"Mineralization (massive to disseminated pyrrhotite, sphalerite, chalcopyrite, pyrite, galena, some silver and molybdenite) forms long narrow conductive zones parallel to the bedding of Archean Yellowknife Supergroup metasediments that define a broad east plunging syncline. Two zones  make up the Turnback Lake showing, the XL zone and the OK zone. The XL zone consists of two en echelon lenses that are 1900 feet long and terminated bynpegmatite and granite.   Work done on this showing includes geological mapping, geochemical sampling, magnetic (ground?) and EM surveys (airborne and ground), trenching and diamond drilling. Resources calculated for the XL zone are listed as diamond drill inferrred at 2,000 ton/vertical foot at 4 oz/T Ag, 0.8% Cu, 4.7% Zn and 1% Pb. The OK zone is reported as being 30x5.3 feet in extent at 18.8 oz/t Ag, 8.4% Pb and 13.7% zinc."
085INW0028,118,1,"The KI pegmatite dyke swarm occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The KI dyke is of the Li-rich variety. It strikes at about 135 degrees and dips steeply to the southeast. It can be traced on surface for about 800 m and is 10 - 15 m thick. There is no marked zonation and the dyke is classified as a simple pegmatite, consisting of 20 - 25% spodumene as 15 cm pale green crystals and, in decreasing order, microcline, quartz and muscovite. The spodumene crystals are generally oriented perpendicular to the strike of the dyke. Hornfelsed wallrock inclusions are common in the southern portion. Drill logs note the development of secondary alteration comprising a fine-grained, aplitic mixture of sericite, albite and hematite.  A reserve of 2 million tons grading 1.4% Li2O based on surface sampling and geological projection to a depth of 500 feet is estimated in AR 080274. One bulk sample taken in 1987 (AR 082495) as part of a program involving the FI pegmatite was submitted for metallurgical testwork. Results indicate that a spodumene concentrate containing 5 - 6% Li2O at an overall recovery of 80% could be produced."
085INW0028,119,2,Production of a high purity lithium carbonate product was achieved using a standard roast and acid leach process. Mica and feldspar by-products were produced by additional flotation steps.
085INW0029,120,1,"The Shorty (Greg) pegmatite dyke occurs in the Yellowknife Basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties. Regional foliation in the area is parallel to sub-parallel to bedding.  The Shorty Li-rich pegmatite intrudes medium grade, turbiditic metasediments. It strikes 037 degrees and dips SW at 50 - 58 degrees. The dyke is 540 m long and averages 23 m in true thickness. A possible faulted extension can be traced for an additional 240 m to the NE. The southern portion of the dyke consists mainly of aplite (albite-sericite?) and narrows with depth along with the central portion. The northern portion maintains its thickness and grade with depth, suggesting that, to some degree, the pegmatite plunges to the north.  The pegmatite is of the simple, unzoned variety although banding consisting of centimetre to metre scale alternations of medium to coarse-grained pegmatite and aplite is common. The aplite may be an albite-sericite alteration common in pegmatites in this area. The dyke is composed mainly of quartz, K-feldspar, spodumene, Na-feldspar and muscovite."
085INW0029,121,2,"Spodumene occurs as white to pale green crystals up to 8 cm long and is preferentially developed in the coarser grained bands where it tends to be oriented perpendicular to banding. However, near the dyke margins, it tends to be oriented parallel to the contact. Muscovite is concentrated near the dyke margins although it is present throughout. Minor amounts of biotite, beryl, tourmaline and cassiterite are present. Assays show that Ta, Be and Sn tend to increase toward the hangingwall of the dyke.  Based on surface sampling, trenching and 11 drill holes totalling 1261.2 m, a drill-indicated reserve of 1.357 million tons grading 1.07% Li2O  has been calculated. The reserve comprises a 400 m long section to a depth of 100 m and assumes a 0.73% Li2O cutoff grade.  The Shorty dyke was apparently called the Greg deposit (NMI) and prior to that was Dyke A of Zone 1 on the Lit claims. Dykes B and C of Zone 1 are parallel to Shorty. B is 240 m NW of Shorty, 330 m long, 3 m wide, and contains medium-grained spodumene throughout. It is noted by Fortier (1947) as a cassiterite occurrence. C is 480 m NW of Shorty, 490 m long, 9 m wide, and carries its best mineralization in the northerly 170 m (Mulligan 1968)."
085INW0033,122,1,"The FI pegmatite dyke swarm lies within the Archean Yellowknife Metasedimentary Basin, a vast area underlain largely by Burwash Formation greywacke-argillite turbidites belonging to the Yellowknife Supergroup (Henderson, 1985). These were intricately folded and faulted during at least two phases of Archean deformation, and metamorphosed to lower amphibolite grade in a 40 km wide, north trending zone. The Burwash sediments were invaded by plutons, plugs and stocks of the Prosperous granite. These discordant and predominantly north-south elongate bodies lie within the amphibolite grade metamorphic zone and include the Hidden Lake stock, 2 km west of the showing.  The FI pegmatite dyke swarm is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with the Prosperous Granite suite. There is a broad zonation in the distribution of pegmatite varieties relative to the larger intrusives in the area: an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta rich varieties and then by Li rich varieties. The FI dyke swarm lies within the Li zone.  The FI swarm contains two main northeasterly trending and vertically dipping dykes known as the Southwest and Main Dykes as well as a number of smaller dykes. Both may be classified as simple pegmatites since internal zoning is not well developed. The Southwest Dyke is discussed in a separate report.  The Main Dyke is a branching granitic pegmatite cutting north striking Burwash sediments. It comprises fine to coarse grained feldspar-quartz-mucsovite with variable amounts of spodumene. Aplitic chill zones, where present, are 15 - 45 cm thick and spodumene poor."
085INW0033,123,2,"The Main Dyke system can be traced for 1800 m along strike but is most continuous along approximately 930 m. This portion is of fairly consistent 20 m width at the north end, and splits into two roughly equal, 425 m long branches in its southern part. The north end is poor in spodumene (5-10%), while the southern part averages about 15% and ranges up to 28%.  The west branch of the southern part is 15.5 m wide and was tested by 6 trenches, concentrated near its south end at approximately 30 m intervals. Spodumene content in the rock exposed in these trenches ranged from 13 to 20%. Assays of 10-pound representative chip samples from the 6 trenches, including chill zones, ranged from 0.66% Li2O across 6.1 m to 2.01% across 6.1 m. Weighted averages across the width of the dyke ranged up to 1.67% across 12.2 m and 1.35% across 18.3 m.  Incomplete sampling in 1975 (AR 080282) allowed a rough estimate of 7.0 million tonnes containing 1.1% Li2O to 152 m depth in the Main Dyke. Unpublished reports referred to in AR 082495 describe a 1978-79 program of drilling and trenching, the results of which formed the basis for a total FI (Main and Southwest Dykes) reserve estimate of 6,530,000 tonnes grading 1.49% Li2O to a depth of 152 m. Of this total, the Main dyke contained 2,424,000 tonnes at 1.54% Li2O.  Five bulk samples taken from the FI dykes in 1987 (AR 082495) were submitted for metallurgical testwork. Results indicate that a spodumene concentrate containing 5 - 6% Li2O at an overall recovery of 80% could be produced. Production of a high purity lithium carbonate product was achieved using a standard roast and acid leach process. Mica and feldspar by-products were produced by additional flotation steps."
085INW0042,124,1,"The showing lies within the Archean Yellowknife Metasedimentary Basin, a vast area underlain largely by Burwash Formation greywacke-argillite turbidites belonging to the Yellowknife Supergroup (Henderson, 1985). These were intricately folded and faulted during at least two phases of Archean deformation, and metamorphosed to lower amphibolite grade in a 40 km wide, north trending zone. The Burwash sediments were invaded by plutons, plugs and stocks of the Prosperous granite, and abundant related pegmatitic dykes and sills. These discordant and predominantly north-south elongate bodies lie within the lower amphibolite grade metamorphic zone, mostly west of the showing. The Hidden Lake stock is exposed 7 km west of the showing.  The showing comprises 5 Li-bearing pegmatite dykes in an area approximately 1 x 1 km. They all strike NE and dip 45 - 70 degrees NW, cutting NE-striking, east dipping, overturned nodular schists of the Burwash Fm. They comprise coarse grained feldspar, spodumene, quartz and minor muscovite, and they commonly branch and contain horses of country rock. Widths given below are surface widths; true widths will be smaller (note the moderate dip). Fortier (1947) notes beryl at this location also; it may be from a small dyke just east of Dyke 12.  Dyke 12, the largest, is 300 m long and up to 7 m wide, but is best mineralized along 200 m where sections up to 4 m wide were estimated to contain 35% spodumene. Banding of 25 cm pegmatitic phases with 2 cm aplitic phases is locally well-developed. Zoning is not evident. Coarse spodumene and feldspar crystals and streaks of grey quartz lie perpendicular to the long axis of the dyke. It contains from 85,000 to 123,000 tons of material, to 30 m depth, grading 1.5% Li2O."
085INW0042,125,2,"Dyke 6 is 1100 m NE of D12, measures 170 x 9 m, and is estimated to contain, to 30 m depth, 85,000 tons grading 1.5% Li2O.  Dyke 5 lies 1200 m NE of D12, measures 158 x 4 m, and is only locally spodumene rich. One sample (AR 080847) contained 2.12% Li2O. Dyke 2 lies 750 m NNW of D12 and is 180 x 1.8 - 9.0 m. Dyke 1 is 900 m north of D12, measures 100 m long by up to 11 m wide, and assayed 0.85 to 1.85% Li2O in 6 samples. These 3 dykes carry 32,000 to 43,000 tons each, totalling 116,000 tons to 30 m depth, grading 15% spodumene, which is the equivalent of 1.0% Li2O (080847)."
085INW0079,126,1,"The showing lies within the Archean Yellowknife Metasedimentary Basin, a vast area underlain largely by Burwash Formation greywacke-argillite turbidites belonging to the Yellowknife Supergroup (Henderson, 1985). These were intricately folded and faulted during at least two phases of Archean deformation, and metamorphosed to lower amphibolite grade in a 40 km wide, N-trending zone. The Burwash sediments were invaded by plutons, plugs and stocks of the Prosperous granite. These discordant and predominantly N-S elongate bodies lie within the higher grade metamorphic zone and include the Hidden Lake stock, 2 km west of the showing.  The FI pegmatite dyke swarm is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, that are probably associated with the Prosperous Granite suite. The pegmatites show a broad zonation in relation to the larger intrusives in the area. An inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The FI dyke swarm contains two main northeasterly trending and vertically dipping dykes known as the Southwest and Main Dykes as well as a number of smaller dykes. Both may be classified as simple pegmatites as zoning is not well developed.  The Southwest Dyke is a tabular, steeply dipping, 030d-striking, granitic pegmatite cutting N-striking Burwash sediments. It comprises 15-25% pale green spodumene as 3-6 cm crystals, 15-25% white and pink microcline as 3-8 cm crystals and 5% muscovite. Between 40% and 60% constitutes secondary alteration consisting of a fine-grained, hematitic mixture of sericite and albite. This material often occurs in alternating ""lateral"" bands with fresher pegmatite and typically carries less spodumene."
085INW0079,127,2,"The dyke can be traced for 610 m along strike and varies from 5-37 m in width. The best grades are in the central section along a length of ~360 m averaging ~25 m in width. Spodumene content in the central portion of the dyke averages 20% and is fairly evenly distributed. Spodumene content decreases northward to 5%, where the dyke contains up to 30% inclusions of country rock and is offset 3 m by a cross-cutting gabbro dyke. The southern portion of the dyke is also less rich in spodumene and appears to be offset 9 m SE from the central portion.  Reserves were estimated in 1975 (AR 080282) from trench chip samples and an assumed depth of 152 m, as 4.7 million tonnes grading 1.4% Li2O. Unpublished reports referred to in AR 082495 describe a 1978-79 program of drilling and trenching, the results of which formed the basis for a total FI (Main & Southwest) reserve estimate of 7,198,000 tons grading 1.49% Li2O to a depth of 500 feet. Of this total, the Southwest dyke contained 4,526,000 tons at 1.46% Li2O.  Five bulk sample taken from the FI dykes in 1987 (AR 082495) were submitted for metallurgical testwork. Results indicate that a spodumene concentrate containing 5-6% Li2O at an overall recovery of 80% could be produced. Production of a high purity lithium carbonate product was achieved using a standard roast and acid leach process. Mica and feldspar by-products were produced by additional flotation steps."
085INW0084,128,1,"The Vo #2 pegmatite dyke occurs in the Yellowknife Basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Vo #2 Li-rich dyke is a member of the Blaisdell Lake pegmatite series. The dyke intrudes medium grade metasediments and is more or less conformable with foliation, striking at 040 degrees with a vertical dip. It is exposed for a strike length of about 250 m and ranges from 7 - 9 m in width. An old description quoted in AR 080283 from GSC Economic Geology Report No. 21 describes the dyke as medium to coarse grained and banded with respect to spodumene distribution. An analogy with other pegmatites in the basin suggests that the banding is due to local secondary alteration to a fine-grained mixture of albite and sericite, commonly referred to as aplite.  Spodumene crystals are oriented perpendicular to the dyke walls. Dark green to black crystals and irregular masses of huhnerkobelite/triphylite are associated with the spodumene. Scattered crystals of beryl are also present. Apatite is reported as abundant in the Blaisdell series (DIAND Contr. to NWT Geol., v3) but is not noted in other reports."
085INW0084,129,2,"A reserve of 138,000 tons grading 1.62% Li2O to a depth of 100 feet was calculated by Canadian Superior Exploration on the basis of surface sampling and geological projection to depth."
085INW0085,130,1,"The Vo #5 pegmatite dyke occurs in the Yellowknife Basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Vo #5 Li-rich dyke is a member of the Blaisdell Lake pegmatite series. The dyke intrudes medium grade metasediments and is more or less conformable with foliation, striking at 040 degrees with a vertical dip. It is exposed over a strike length of about 260 m and has an average width of about 25 m. An old description quoted in AR 080283 from GSC Economic Geology Report No. 21 describes the dyke as indefinitely banded, with aplitic (sericite-albite alteration) phases. Better grades of spodumene are found in the coarser grained portions of the dyke and grade diminishes towards the southwest end, where aplite is more abundant. Small white beryl crystals are fairly common near the north contact, in association with quartz and pink cleavelandite. One greenish mass was tentatively identified as triphylite. Apatite is reported as abundant in the Blaisdell series (DIAND Contr. to NWT Geol., V.3) but is not noted in other reports.  "
085INW0085,131,2,"A reserve of 150,000 tons grading 1.55% Li2O was calculated in 1975 by Canadian Superior Exploration based on six surface samples and geological projection to a depth of 100 feet. The same company drilled two short holes in 1978 showing that the dyke narrows somewhat with depth. No new reserve was reported."
085INW0104,132,1,"Mahe is a gold-bearing, quartz breccia hosted in a folded, carbonaceous, sulphide-rich siltstone.  The showing is situated in Archean aged rocks of the Yellowknife Supracrustal Belt.   Exploration work, including both surface and undergrounding drilling,  has defined the deposit size as being 305 metres long, 6 to 30 metres wide and extending to a depth of 121 metres (GNWT RWED, MOG Book (1997)).."
085INW0105,133,1,"This showing has been subjected to intermittant exploration from 1938 to 1987 in the form of: geochemical sampling, geological mapping, diamond drilling and in 1974 a 350 foot deccline was driven with one level (250 feet) and sampling. In 1984-85, trenching, sampling and diamond drilling was done and, in 1987, diamond drilling, geophysics and decline rehabilitation took place. Resources calculated (1974) are listed at 64,265 tons at 0.157 oz/t gold and some(?) silver.  In this showing gold is associated with sulphides (arsenopyrite-pyrrhotite-galena-pyrite-chalcopyrite-and sphalerite) in elongated quartz masses and stockwork, spatially related to a S-shaped fold near a fault in the greywacke and slates of the Archean Yellowknife Supergroup."
085INW0142,134,1,"The Mitchell Lake showing has been subjected to strippong, trenching, diamond drilling and bulk sampling. Resources calculated (possible) are listed as 3,000 tons at 1.5 oz/t gold to 120 feet.  Gold mineralization is in shear hosted quartz veins in schists and argillites of the Archean Yellowknife Supergroup. Visible gold is present in a mineralized lens in the No. 1 zone. This lens, having a width of 3 m and a length of 10 m is located within the nose of a drag fold. Gold mineralization is associated with pyrite and arsenopyrite."
085INW0155,135,1,"Gold mineralization occurs within quartz veins in sediments within the Archean Yellowknife group. This showing has been subjected to various forms of exploration since 1937 which included geochemical sampling, trenching, and diamond drilling. A decline was driven on the Lambert vein and a bulk sample was taken in 1987. Three separate veins with resources are as follows: Lambert Vein: 100ft x5.1 ft at 0.663 oz/t gold(1966), No. 14 vein: 110ftx4.3ft at 0.416 oz/t gold (1986) and No. 18 vein: 320ftx5.4ft at 0.278 oz/t gold (1986)."
085INW0158,136,1,"Pegmatite  dykes containing beryl cut a granite plug and associated metasediments of the Archean Yellowknife Supergroup. Pegmatite mineralogy consists of quartz-feldspar-beryl-tourmaline and minor columbite-tantalite, apatite and Mn-alluaudite. This showing has been subjected to trenching and shallow diamond drilling."
085ISE0001,137,1,"The Best Bet pegmatite dyke occurs in the Yellowknife metasedimentary basin within the  Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Best Bet pegmatite is a Li-rich variety belonging to the Faulkner Lake series. It is approximately 100 metres long and up to 8 metres wide. It strikes 010 degrees with a steep westerly dip and is roughly concordant with foliation in the enclosing schist. Some shearing has taken place along the hangingwall contact. The pegmatite is well-zoned internally, with the following sequence from core to border:  core: quartz - muscovite - K-feldspar core intermediate zone: K-feldspar-quartz-spodumene-muscovite wall zone: quartz-plagioclase-muscovite border zone: fine-grained quartz-muscovite.    "
085ISE0001,138,2,"In addition to the above minerals, it also contains beryl, columbite-tantalite, amblygonite and Li-muscovite. Much of the plagioclase has a cleavelandite habit. Most of the plagioclase-muscovite assemblage is metasomatic and the beryl and columbite-tantalite tend to be associated with it. Spodumene crystals and blocks of amblygonite in the central core reach sizes of up to 2 metres and 1 metre long respectively.  The pegmatite was mined in the past for its tantalite-columbite content.  Estimates of spodumene content range from 25% in the northern half of the pit to about one-half of this in the southern half. Average Lithium Oxide contents for the spodumene are reported to be 6.49%.  In 1975 Canadian Superior Exploration claimed that the pegmatite had a potential resource of 42,700 tons at 2.0 % Lithium Oxide to a depth of 500 feet.  Other higher grade, lower tonnages have been estimated by other companies from limited drilling of the pegmatite."
085ISE0002,139,1,"The Moose #2 pegmatite dyke and smaller Moose #1 dyke occur in the Yellowknife Sedimentary Basin within the Slave Structural Province. They are members of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites are most abundant in Burwash Formation sediments where the sediments have been metamorphosed to lower amphibolite facies. There is a broad zonation in the distribution of pegmatite varieties relative to the larger intrusives in the area: an inner zone dominated by Be-rich pegmatites is closest to the intrusion, and is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties. The Moose dykes are Li-rich varieties and are members of the Faulkner Lake series.  The two dykes are 1600 metres apart and appear to be aligned along the same structure. The #2 dyke strikes northerly and dips steeply to the west. It is about 420 metres long and up to 60 metres wide at surface. A 221 metre strike length was drilled to a 30 metre depth, showing the average thickness at that level to be 7.5 - 9 metres. The #1 dyke is slightly less than 300 metres long with a maximum thickness of 10 metres. Both are internally zoned as follows: core is quartz-spodumene-amblygonite;  wall zone is Kspar-quartz-muscovite-cleavelandite;  border zone is quartz-muscovite.  Other minerals present include schorl tourmaline, beryl, cassiterite, petalite and lithiophyllite. Li mineral rich and Cb-Ta mineral rich zones are largely mutually exclusive."
085ISE0002,140,2,"The former are concentrated in or near the central core while the latter are concentrated in two feldspar-rich zones near the walls and in the fine-grained border zone. The distribution of columbite-tantalite is also zoned, with a blocky Ta-rich variety concentrated in the border zone and a platy Cb-rich variety elsewhere. Beryl tends to occur as white irregular crystals and masses on the order of 20 cm across within the wall zone bordering the core.  The quartz core is particularly well-developed in the #2 dyke, reaching a width of about 4 metres. Large crystals and blocks of spodumene and amblygonite reach sizes of up to 2 metres and 1 metre respectively. Patches and stringers of metasomatic albite and secondary muscovite are found throughout the body.  The deposit has been mined on two occasions, the first time involving intermittent production in the period 1946-52 by De Staffany Tantalum-Beryllium Mines Ltd. who produced a heavy mineral concentrate. Boreal Rare Metals Ltd. mined the deposit in the winter of 1953-54 for both heavy minerals and amblygonite. Beryl was stockpiled during this period. Remaining reserves are estimated at 700,000 tonnes grading 7.44% Li and 0.25% Cb (Northern Miner, 05/06/80)."
085ISE0003,141,1,"The Lens pegmatite dyke occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Lens pegmatite is a Li-rich variety belonging to the Buckham Lake East series. It is about 90 m long and up to 20 m wide. It parallels foliation in the enclosing metasediments (quartz-biotite-cordierite schists) and strikes north-northwesterly with a vertical dip. Internal zoning is not well-developed. It appears to be the most spodumene-enriched pegmatite in the series, consisting of 25 - 30% green spodumene crystals, up to 0.5 m long, that tend to be perpendicular to the trend of the dyke, and up to 40% secondary alteration products comprising a finer-grained mixture of albite and muscovite. The remainder of the dyke is made up of quartz and muscovite. Minor amounts of beryl and columbite-tantalite are associated with the secondary alteration minerals.  A paramarginal resource of 102,600 tons grading 1.97% Li2O has been estimated from surface sampling of the Lens pegmatite (Lasmanis, 1978)."
085ISE0004,142,1,"The Mut pegmatite dyke occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The pegmatite is a member of the Li-rich Buckham Lake East series. The dyke conforms with foliation in the country rock, striking at 050 degrees with an apparently vertical dip. It is about 80 m long and averages 5 m in width. Most of the pegmatite is homogeneous and contains 25-35% spodumene in rather evenly distributed green crystals up to 30 cm in length. These tend to be oriented perpendicular to the contacts. Spodumene content decreases where the dyke pinches out at near its ends. Another 40% of the dyke is made up of white and pink microcline feldspar with crystals up to 60 cm in length. Quartz pods situated near the centre probably represent a segmented quartz core zone. Approximately 15-20% of the dyke has been affected by secondary alteration involving the development of a mixture of pink, fine-grained sericite and albite, particularly near the contacts. No Be, Cb-Ta or Sn minerals have been found to date.  A reserve of 25,000 tons grading on the order of 2.2% Li2O was calculated by Canadian Superior Exploration Ltd. on the basis of surface sampling and geological projection to a depth of 100 feet."
085ISE0005,143,1,"The Bin pegmatite dyke occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The pegmatite is a member of the Li-rich Buckham Lake East series. It strikes at about 060 degrees and although an exact dip is not reported, it appears to be steep. The dyke is about 125 m long, averages 12 m wide and has been offset about 20 m into two separate bodies. The western segment contains more than 25% spodumene, 35% white microcline as crystals up to 45 cm across, 15% quartz and 5% muscovite in books up to 3 cm across. About 10% of the dyke has been affected by secondary alteration to a fine-grained mixture of sericite and albite. Minor amounts of beryl and columbite-tantalite are reported to be associated with the secondary minerals. The eastern segment appears to contain somewhat less than 25% spodumene but otherwise is similar to the western one.  A reserve of 99,000 tons grading 1.75% Li2O was estimated by Canadian Superior Exploration Ltd. on the basis of one chip sample and geological projection to a depth of 100 feet (AR 080278)."
085ISE0006,144,1," The Thor Lake deposits are situated in the alkaline Blatchford Lake Plutonic Complex which intrudes Archean plutonic rocks and Archean metasediments of the Yellowknife Supergroup at the southern margin of the Slave Province. Geological mapping by Davidson (1972, 1978) led to the recognition of several units that make up this multiphase, sub-circular ring complex, some 23 km in diameter and 235 square km in area. Successive units range from gabbro, with anorthosite inclusions, through leuco-ferrodiorite, quartz syenite and granite, to peralkaline granite and syenite (Davidson, 1982).  It is convenient to consider the Blatchford Lake Complex in two parts: the earlier, western part including the Caribou Lake gabbro, Whiteman Lake quartz syenite, Hearne Channel granite and Mad Lake granite, and the later, more extensive Grace Lake granite with its Thor Lake syenite core. Rare element minerals are enriched in the later peralkaline unit.  Isotopic determinations indicate an early Aphebian age (2150 Ma) for the Complex (Davidson, 1982). Bowring et al. (1984) obtained U-Pb zircon ages of 2175 +/- 7 Ma for an older alkaline phase (Hearne Channel Granite) and 2094 +/- 94 Ma for the younger peralkaline phase, the Thor Lake syenite.  Mineralization is developed in the central core of the complex which is referred to as the Thor Lake Syenite, a 30 square km oval in the centre of the Grace Lake Granite pluton. Six varieties of syenite including a pegmatitic phase have been identified on the basis of textural and compositional differences. In the vicinity of the mineral deposits, the syenite consists of a massive medium to coarse grained assemblage of K-feldspar with interstitial sodic amphibole, magnetite and minor quartz."
085ISE0006,145,2,"An area of late stage veining, alteration and mineralization is centred on Thor Lake in the western part of the Thor Lake syenite. This area contains five zones of Nb, Ta and REE enrichment along with high concentrations of Zr, Ga, Be, F and locally Y, Th and U. Only the Lake and T zones are of potential economic interest.  Lake Zone The Lake Zone is a 2 square km, triangular-shaped area of dark, altered and brecciated rock beneath and south of Thor Lake. It is the largest of the five mineralized zones and contains Nb, Ta, REE, Y and Zr. Two main alteration types are present: 1) an albitite and K-feldspar-rich syenitic pegmatite resembling a chaotic breccia that has been intensely metasomatized; and 2) a diverse suite of rocks rich in mafic minerals such as aegirine, biotite, Fe and Ti oxides, albite, K-feldspar and quartz. Accessory minerals include zircon, fluorite, allanite, ferro-columbite and members of the bastnaesite-group. The mafic rocks are also brecciated but alteration is more intense. A body of nepheline syenite including minerals such as sodalite, pectolite, analcite, catapleiite, eudialyte, andradite, willemite, mesolite and natrolite has been identified below the Lake Zone. It is in part altered, but is not enriched in incompatible elements and is believed to be a late stage intrusion. Twenty-nine drill holes in the Lake Zone have outlined a resource of 65 million tonnes grading 0.03% Ta, 0.4% Nb, 1.7% combined REE and 3.5% Zr (Trueman et al., 1988).  T Zone The T Zone trends north-northwest away from the Lake Zone for approximately 1 km, is up to 275 m in width and extends to a depth of 150 m. It straddles the Grace Lake Granite-Thor Lake Syenite contact and offsets it."
085ISE0006,146,3,"Near the Lake Zone, it is dyke-like and is known as the South T Zone. The northern end, known as the North T Zone, is a small circular body. Some 15 lithologies arranged in concentric to sub-horizontal shells have been recognized in the T Zone and have been grouped into four zones. The T Zone is of particular interest for its Be content.  The outermost Wall zone is a pink to buff weathering, massive unit of variable texture dominated by relict microcline, albite and minor quartz. Columbite is a common accessory mineral and high levels of gallium are associated with feldspars in which it substitutes for trivalent aluminum. Moving in, the Lower Intermediate zone includes five lithologies consisting of various proportions of quartz, biotite, feldspar, chlorite and magnetite. Beryllium is present in the mineral phenacite. Yttrium and rare-earth elements are in an intimate admixture of a metamict species believed to be thorite. Niobium is in the mineral columbite, which occurs as massive, granular and radiating spicular aggregates. Other minerals include purple fluorite and dolomite.  The Upper Intermediate zone is transitional between the Lower Intermediate and central Quartz zones and is similar in gross mineralogy to the former. It differs in that polylithionite and phenacite are particularly abundant, making this zone the most important host for beryllium. Polylithionite is of interest for its lithium and rubidium content. Other Be minerals include bertrandite, gadolinite and helvite. Y and REE are present in bastnaesite-group minerals, thorite and Th-Y silicates.  The Quartz zone occupies the core of the North T Zone and is present in patches within the South T Zone. It is essentially monomineralic, consisting of white and greyish translucent quartz."
085ISE0006,147,4,"A total of 124 drill holes in the T Zone has outlined 1.6 million tonnes grading 0.85% BeO, including 435,000 t of 1.4% BeO, 0.26% Y2O3, plus Nd, Sm, Gd, and Ga.  Fluorite Zone The Fluorite zone is located at the southeastern end of the Lake Zone. It is approximately 150 m in length, up to 15 m wide and consists of a dense, dark-brown siliceous rock with occasional pods of fluorite. Accessory minerals include zircon, xenotime, allanite and members of the  bastnaesite-group.  R Zone The R zone is a series of pegmatitic lenses and patchy zones of albitization in foliated syenite. It is about 4 km long, up to 30 m wide and is locally enriched in Be, Th, Nb and REE.  S Zone  The S zone is subparallel to the R zone and lies about 200 m north of it. It is 300 m long, averages 10 m in width and consists of syenite altered to albite and albite-polylithionite. Patchy enrichments of Be, U, REE, Y and particularly Nb in ferro-columbite are present.  The Thor Lake area was first staked for uranium and REE in 1970. In 1976, Highwood Resources discovered anomalous levels of Nb and Y as well as REE.  By 1985, a 500 m long decline had been driven into the North T Zone to facilitate bulk sampling for metallurgical testing and related marketing studies. A feasibility study was completed in 1989, after which Highwood's joint venture partner Hecla Mining Co. decided to withdraw from the project, citing difficulties in securing commitments from potential customers. The deposits remain one of the largest beryllium reserves in the western world."
085ISE0012,148,1,"The Hid pegmatite dyke occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Hid pegmatite is a Li-rich member of the Buckham Lake West series. The dyke is approximately 200 m long, up to 6 m wide and is discontinuous. It strikes at 070 degrees and dips steeply to the north, crosscutting foliation in the enclosing cordierite quartz biotite schist. The pegmatite is poorly zoned, with microcline, quartz and muscovite as the dominant gangue minerals. Spodumene constitutes 20-25% by volume. Irregular but strong albitization is present.  A reserve of 50,000 tons grading 1.56% Li2O has been calculated on the basis of two surface samples and geological projection to a depth of 100 feet (AR 080275)."
085ISE0013,149,1,"The Mac or McDonald pegmatite dyke occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Mac pegmatite is a Li-rich member of the Buckham Lake West series. The dyke is 120 m long and averages 10 m in width. It strikes 280 degrees, dips 60 degrees to the south and appears to be conformable with foliation in the enclosing cordierite quartz biotite schist. Zoning is well-developed, particularly in the central parts of the pegmatite, with the following sequence beginning in the core and moving outwards:  1. quartz-muscovite core  2. Kfeldspar-quartz-spodumene-amblygonite-muscovite  3. quartz-plagioclase-spodumene-muscovite  4. quartz-plagioclase-muscovite  5. quartz-muscovite-plagioclase border zone.  The intermediate zones are the largest by volume and the core is discontinuous, consisting of a number of separate lenses. Muscovite-rich zones are thicker in the hangingwall area. Alteration in the form of a mixture of albite and sericite is common, particularly in the central part of the dyke.  "
085ISE0013,150,2,"Individual spodumene crystals in the Mac dyke reach lengths of 3 metres and most are larger than about 30 cm. There is a tendency for these to be oriented perpendicular to dyke contacts. The spodumene is relatively fresh compared with that in many of the other dykes in the area. In addition to the lithium minerals noted above, Jolliffe has described minor quantities of lithiophyllite. Notable quantities of white beryl and both fine-grained equant and platy columbite-tantalite are associated with the albite-sericite alteration.  A reserve of 73,000 tons grading about 2% Li2O has been estimated on the basis of two chip samples, visual estimates and geological projection to a depth of 100 feet (AR 080276). Although no assays of Ta/Nb are available, Jolliffe noted several areas within the dyke, ranging in size from three to ten square feet, in which he estimated between 1 and 2 percent tantalite."
085ISE0017,151,1,"The Norma gold prospect is situated in the Yellowknife Basin, a supracrustal belt within the Archean Slave structural province. Gold occurs in quartz veins hosted by turbiditic metasediments belonging to the Burwash Formation which is part of the Archean Yellowknife Supergroup. The sediments include medium-bedded greywackes rhythmically interbedded with argillite and occasional layers of grey to black, thin-bedded phyllite. The strata are strongly deformed into folds with axes plunging steeply to the northeast. Regional metamorphic grade is lower greenschist.                      The Norma vein has been traced on surface for about 550 m. It averages 15 cm in thickness and is concordant with bedding, following an argillite layer in the turbidites. Several minor quartz veins parallel it nearby. It is composed mainly of rusty weathering, grey quartz containing a variable amount of wall rock inclusions along with minor carbonate, feldspar, biotite and chlorite. Metallic minerals constitute less than 1% of the vein by volume and include arsenopyrite, galena, chalcopyrite, marcasite, scheelite and native gold. Sphalerite and pyrrhotite have been tentatively identified. Native gold tends to occur with galena and the other sulphide minerals, particularly near the slate wall rock, near inclusions of wall rock, and in chloritic slips.                      The bulk of better grade material is present in two main shoots named the ""A"" and ""B"". The A shoot plunges parallel to the dip of the vein at this point, at NNE/70 degrees. At surface, the A shoot was reported to be 2.5 m long and 0.5 m wide with a grade of 1.64 oz/ton Au. At the 175 foot level, it was reported to have a drift length of 7 m, width of 0.5 m and grade of 0.55 oz/ton Au."
085ISE0017,152,2,"Much of the hangingwall argillite in its vicinity has been strongly chloritized, while silicification of the footwall greywacke appears to have taken place. Also in the footwall is a 20 m wide area in which the sedimentary strata have been strongly contorted, broken and infilled with numerous stringers and irregular bodies of quartz. Shoot B was reported to be about 10 m long, 0.3 m thick and to contain in excess of 1 oz/ton Au. Shallow diamond drilling revealed only erratic values of gold.  Discovered in 1939, the prospect has received much exploration attention since then. High surface assays and heavily promoted results of a drill program led to a premature and abortive attempt at production in 1946 with a reserve estimate of 105,000 tons grading 1.0 oz/ton Au. A total of 252 tons were eventually milled with a production of 7.5 oz gold. In 1947, an independent consultant (A.D. Hellens) was called in and calculated a new reserve of 1,200 tons grading 0.65 oz/ton Au to a depth of 225 feet."
085ISE0021,153,1,"The Thor (Echo Lake, Tanco) pegmatite dyke swarm occurs in the Yellowknife Basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Thor swarm is a Li-rich member of the Thor-Echo series. Numerous northwest striking and steeply to vertically dipping pegmatite dykes occur in an area about 1200 m long and 650 m wide. Both zoned and unzoned types are present although the latter are most common. They have been divided into four groups as follows:  WEST  Approximately 45 m long and up to 5 m thick, this dyke is well-zoned, grading from a quartz - spodumene ? K-feldspar core through a plagioclase - K-feldspar - muscovite - quartz ? spodumene intermediate zone to a plagioclase - muscovite - quartz wall zone. Spodumene crystals are generally oriented perpendicular to the contacts. Alteration to a fine-grained mixture of albite and sericite is widespread. Beryl, columbite-tantalite, apatite and altered triphylite are associated with alteration.  TANCO  This dyke lies along strike from the WEST dyke and is about 180 m long and up to 8 m wide. It is relatively homogeneous, consisting mainly of quartz, albite and minor muscovite."
085ISE0021,154,2,"Blocky K-feldspar, spodumene and amblygonite are dispersed throughout the dyke but are more abundant in the central portions. Beryl and columbite-tantalite are generally found with them.  CENTRAL  This swarm consists of two sets of dykes with slightly differing orientations. A northwest trending set is generally unzoned, with spodumene and K-feldspar oriented perpendicular to dyke margins. Alteration to fine grained albite-sericite is present although beryl, columbite-tantalite and phosphate minerals are rare. A northeast trending set of dykes connects or bridges the northwest set and is characterized by unoriented K-feldspar and spodumene as well as a lack of alteration and the absence of rare element mineralization.  EASTERN  The eastern set strikes northwesterly and dips steeply to the northeast. Internal structure varies from completely unzoned to well-zoned along the length of the dykes. Spodumene content varies from abundant to absent and Nb-Ta and Be mineralization is rare.  Various phases of exploration have been carried out since the mid-1950's, including trenching, bulk sampling and some diamond drilling. A reserve of 1.84 million tons grading 1.5% Li2O based on surface sampling and geological projection to a depth of 100 feet has been calculated by Canadian Superior Exploration (AR 080478)."
085ISW0007,155,1,"The Big Hill East pegmatite dyke swarm, also known as the BA or Murph, occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Big Hill East pegmatites are Li-rich varieties occuring in a northeasterly trending dyke swarm that cuts the trend of bedding in the host metasediments at a low angle. The swarm has a strike length of 1070 m and a width of about 150 m. Individual dykes are up to 15 metres wide. Immediately north of this swarm, the Big North swarm probably represents a faulted off extension of the Big Hill East.  The pegmatites are classified as simple rather than zoned, since crystals are generally a few centimetres across and the various minerals are distributed relatively evenly throughout. In order of abundance, the minerals present are: microcline, spodumene, quartz and muscovite. In the larger dykes, spodumene generally occurs as pale green crystals averaging 8 cm in size which tend to be oriented perpendicular to the contacts and dip east at 10 - 30 degrees. However, both microcline and spodumene occur as crystals up to 0.5 m across locally. A secondary, fine grained plagioclase-muscovite alteration is common, constituting as much as 30% of the dykes in places."
085ISW0007,156,2,"Where present, it has also affected spodumene and greatly reduced its abundance. The alteration is particularly common where dykes finger out and may be somewhat more abundant in the Big North swarm.  Reserves are estimated (AR 080273) at 3.1 million tons grading 1.5% Li2O to a depth of 150 m. One old drill hole from the 1950s (AR 082348) showed the dykes to remain constant in width to that depth. At the Big North swarm, the same report estimates a reserve of 160,000 tons grading 1.27% Li2O to a depth of 30 m."
085ISW0009,157,1,"The Jake pegmatite dyke swarm occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Jake dyke swarm consists of 15 generally northwesterly striking pegmatite dykes of the Li-rich variety, each up to 5 m wide and 1000 m long and all contained within an area about 1 km by 1.2 km. Unlike many of the other members of the Yellowknife pegmatite field, these are hosted by intrusive granodiorite of the Defeat Plutonic Suite rather than metasediments. The dykes are immediately northeast of the Paint dyke swarm and may in fact be related to them.  Although some of the dykes exhibit a quartz core, in general they are not well-zoned and can be classified as simple. Mineralogy is similar throughout the swarm although the proportions of minerals in each vary to some degree. The Jake #1 dyke is described in most detail and consists mainly of white, euhedral feldspar, quartz and muscovite together with about 10% spodumene and minor amblygonite. Spodumene occurs as colourless to pale green-grey, zoned crystals up to 30 cm long that are generally oriented perpendicular to the contacts with host granodiorite."
085ISW0009,158,2,"Spodumene tends not to occur in the margins of the dyke. Amblygonite is greyish-white and typically contains small amounts of pale blue lazulite. Feldspar crystals occasionally contain minor amounts of platy tantalite-columbite. Other minor accessory minerals include yellow-green apatite, galena, cassiterite and possible wolframite.  Five of the thirteen dykes contain significant amounts of spodumene. A 1981 assessment report (AR 081352) calculates a reserve of approximately 2.1 million tonnes grading 1.12% Li2O on the basis of surface sampling, visual estimation and geological projection to a depth equivalent to 1/2 of the sampled strike-length (maximum of 380 m). Two more dykes were described as potentially interesting but having lower visual estimates of grade."
085ISW0010,159,1,"The Paint pegmatite dyke swarm occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Paint Li-rich dyke swarm consists of four northwesterly striking and steeply southwesterly dipping pegmatite dykes up to 1.6 m wide and 1000 m long. Unlike many of the other members in the Yellowknife pegmatite field, they are hosted by intrusive granodiorite of the Defeat Plutonic Suite rather than metasediments. They are immediately southwest of the Jake swarm and may in fact be related to them.  The spodumene-bearing dykes are not zoned and may be classified as simple, although a number of smaller, non-lithium rich dykes in the vicinity are well-zoned. The gangue mineralogy of the dykes is not discussed in available references other than mentioning the presence of pink feldspar. Spodumene and much lesser amblygonite are the only potentially economic minerals.  Accessory minerals include columbite-tantalite, sphalerite, galena and cassiterite. Spodumene occurs as large, light green crystals usually oriented at high angles to dyke contacts. On surface, these have been altered to a chalky white colour."
085ISW0010,160,2,"Amblygonite occurs in amounts of up to 5% as small patches lacking crystal form. It is also found in one of the smaller, zoned and presumably unrelated pegmatites.  A reserve of 2.774 million tonnes grading 1.75% Li2O was calculated in AR 081137 on the basis of crystal counting (with some check assays) and geological projection to a depth of 500 m. A 100 kg bulk sample was submitted to Lakefield Research for metallurgical testing. The results showed that a high grade lithium concentrate assaying 6.2% Li2O could be produced at a recovery of 87%."
085ISW0011,161,1,"The Ann (Reid Lake) pegmatite dyke occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite. The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Ann dyke is a Li-rich variety. It strikes at 130 degrees, dips steeply to the south and is roughly conformable with foliation in the enclosing metasediments. It has been traced on land and under a lake by drilling for a strike length of 1200 m and has an average thickness of 12 m. The pegmatite is unzoned, consisting of grey plagioclase, milky to grey quartz, a variable amount of pink feldspar and scattered books of muscovite. Spodumene occurs as platy greenish grey crystals up to 25 cm long. Amblygonite is reported and the presence of high Li2O assays in the absence of spodumene suggests that it may be relatively abundant.  Drilling in 1956 (AR 082243) intersected the dyke at depths of over 100 m and demonstrated continuity in width and grade. A possible reserve of 3,335,600 tons grading 1.92% Li2O is reported in Canadian Deposits Not Currently Being Mined (1989); estimate is from Lasmanis (1978)."
085JNE0002,162,1,"The Cassidy Point deposit lies near the western edge of the Archean Yellowknife Metasedimentary Basin, a vast area underlain largely by Burwash Formation greywacke-argillite turbidites belonging to the Yellowknife Supergroup (Henderson, 1985). These were folded and faulted during at least two phases of Archean deformation, and metamorphosed to lower amphibolite grade in a 40 km wide band including the Cassidy Point deposit. The deposit lies approximately 3 km west of a north-south elongate pluton belonging to the Archean Prosperous granite, which is a group of plutons and smaller bodies of massive, unmetamorphosed granite, and abundant related pegmatite dykes.  The deposit is an auriferous quartz vein system within a shear, cutting folded metagreywackes and incipiently nodular schists of the Burwash Formation. The sediments in the southern Prosperous Lake area have been folded about moderately to gently SE-plunging and moderately to steeply NW-plunging axes, while the auriferous zone trends NE/40 degrees NW (MIR 81). According to AR 081344, the veins occupy a shear folded into a syncline plunging gently along an east-west axis; this plunge, and the dips of the shear ""limbs"", are not conformable with bedding, suggesting that the shear cross-cut the beds prior to folding. According to NMI, the main zone or Zone No. 1, comprising sheared quartz-mica schists, quartz lenses, sphalerite and pyrite (with minor pyrrhotite, galena and visible gold), strikes NW to N and dips 60 degrees W, is 0.6 m wide in the northernmost 20 m and thickened in the nose of a small syncline to 4.5 m wide in the southern 15 m. There are also a No. 2 Zone a metre or so to the west, with a W/77 degree N attitude, and a No. 3 Zone to the south striking NW."
085JNE0002,163,2,"Numerous grab samples from the main pit have assayed over 30 g/t Au. Typically, gold values increase with sphalerite content, and a 0.5 m drill intersection in 1955 assayed 26 g/t Au and 4.4% Zn. A 0.2 m intersection assayed 32 g/t Au and 26.2% Zn, and a 1.2 m section assayed 0.12% Zn, 2.4% Pb and 20 g/t Au.  A bulk sample weighing 1112 tonnes was taken from a decline driven into the main vein in 1986, and was processed at the Con mill, where a 97.12% recovery was attained. The ore averaged 12.7 g/t Au. The latest reserve estimates are from 1981 (AR 081344) and state proven reserves of 1400 tonnes grading 15.43 g/t Au, amenable to open pit mining with a strip ratio of 4:3."
085JNE0011,164,1,"The Vega showing or deposit lies near the western side of the Archean Yellowknife Metasedimentary Basin, a vast area underlain largely by Burwash Formation greywacke- argillite turbidites belonging to the Yellowknife Supergroup (Henderson, 1985). These were folded and faulted during at least two phases of Archean deformation (Fyson 1987, Brophy 1987), and metamorphosed to lower amphibolite grade in a 40km-wide band including the showing. The showing lies ~2.5km SW of a N-S elongate pluton belonging to the Prosperous granite, which is a group of plutons and smaller bodies of massive, unmetamorphosed granite, and abundant related pegmatite dykes, which invaded the Burwash sediments in the late Archean.  Jolliffe (1941) shows a Au occurrence in a NW-trending vein on the south side of McKeekan Bay, the southern bay of Prosperous Lake (GSC Map 868A). Assessment records show that trenching and drilling tested two quartz veins here in 1944, one of the south side of Mckeekan Bay striking NW for 128m, and one on the north side, 300m NNE of the first, striking WNW for 106m. The northern one was opened in 5 trenches. Another trench tested a target inbetween the two veins (another vein?). The southern quartz vein coincides with Jolliffe's gold occurrence and was tested with 6 trenches. Five holes were drilled along 400m including the south vein and the area to its north. A sixth drill hole was collared on a small island in the Bay roughly 750m SE of the vein exposure.  Results of this work are not available, but in a report dealing with the Tom and Ptarmigan Mines property, 1500m SW of Vega, the Vega is referred to as a deposit for which small reserves of gold ore were outlined, presumably in the late 1940s."
085JNE0011,165,2,"Nearby deposits such as Tom, Ptarmigan and Cassidy Point are hosted by discordant quartz veins mineralized with pyrite, sphalerite, galena and locally other sulphides, cutting turbiditic metasediments near NNW-trending, Early Proterozoic sinistral faults."
085JNE0044,166,1,"The showing occurs in the Yellowknife (YK) Volcanic Belt. This Archean supracrustal belt trends north for roughly 8.5 km and includes a 10 - 12 km thick, tholeitic basal sequence, the Kam Group, overlain by 2 km of dominantly calc-alkaline volcanics and turbiditic sediments of the Banting Group. The volcanic belt is a SE-facing, steeply dipping homoclinal sequence, flanked on the east by a vast basin of Archean turbiditic metasediments, intruded to the west by the Archean Western Plutonic Complex, and cut by Proterozoic diabase dykes of the Dogrib and Indin generations. Regional metamorphism in the belt does not exceed greenschist facies, except adjacent to the Western granodiorite. The entire belt has been subjected to compressional stress that is manifested by anastomosing, high-angle, reverse shear zones (Lewis 1987, MDD GAC YK Field Guide p191). These early shears are pre-diabase in age, and host most of the gold mineralization discovered to date in the belt. A set of regional, Proterozoic sinistral faults post-date the diabase; one of these is the Akaitcho Fault, which strikes NW just south of the deposit.  The four formations of the Kam Group comprise predominantly mafic volcanics with minor amounts of dacitic volcanics and tuffaceous sediments, intruded by metagabbro sills and sheeted dykes. The Crestaurum Formation, second from the base, is regionally characterized by massive and pillowed basalts or andesites with a number of laterally continuous felsic horizons, invaded by synvolcanic(?) metagabbro sills and cut by a N-trending swarm of metagabbro dykes (Padgham 1987; MDD GAC YK Field Guide p11). The overlying Townsite Formation, on the other hand, comprises dacitic pyroclastics intruded by metagabbro dykes and sills, particularly one large sill which invaded the central part of the Formation."
085JNE0044,167,2,"On the property, the stratigraphy strikes 030 - 050 degrees and dips 70 - 85 degrees east except in the vicinity of the west zone where dips are 75 - 85 degrees west.  At the showing, massive, pillowed and variolitic andesites of the Crestaurum have been noted in the hangingwall of the west zone. Porphyritic dacite and the major, central gabbro sill of the Townsite Formation form the footwall, and a younger? (AR 082156) gabbro of the Townsite Formation hosts the east zone. The volcanics have been metamorphosed to lower greenschist facies, consisting of chlorite and epidote after hornblende, hornblende after pyroxene, and epidotized feldspar.  The anastomosing shear system which hosts the ore at Giant Mine, to the south, is apparently displaced 1900 m NW by the Akaitcho Fault, to continue as the Lynx west zone. The Lynx shear system has been described as a west-dipping west zone, and a subsidiary, gently east-dipping east zone, forming an anticlinal geometry similar to that seen at Giant Mine, but with the crest of the anticline removed by erosion. The Lynx deposits occur north of Gold Lake and south of Vee Lake, but the NT MINFILE showing Supercrest GKP Zone, just south of Gold Lake, partially underlies the Lynx property and is geologically part of the Lynx system.  The east zone shear strikes NE and dips 20 degrees SE. About 100 m north of Gold Lake, where the shear is approximately 100 m wide, a SW-plunging synclinal undulation in it hosts the Original Discovery. The Discovery comprises two strongly sheared, carbonatized and silicified auriferous zones along the boundaries of the shear. South of the Original Discovery, the Lynx Fault, a west-trending dextral splay of the Akaitcho Fault, probably displaces the zone 275 m west, from which point it continues south to the Akaitcho Fault (AR 082156)."
085JNE0044,168,3,"Its total length is roughly 730 m, and it has been traced down-dip an unknown distance. About a kilometre NE of the Discovery, minor gold values are present in chlorite-sericite schists in the NE extension of the east zone (NMI Au 09). Grades and sizes in the east zone were sub-economic in 1965 (AR 082156).  The west zone occurs along the locus of the Vee Lake fault, an early (pre-diabase) thrust fault with unknown vertical displacement and 1500 - 3000 m horizontal displacement. It strikes 010 - 020 degrees and dips 70 - 75 degrees west, partially along the west side of the Townsite central gabbro sill and partially along the Townsite - Crestaurum contact. The fault extends 7 km, from the Akaitcho Fault south of Gold Lake, through Vee Lake to the Hay-Duck Fault at Jackson Lake, and is variably sheared along its length. It crosses through Townsite dacites and metagabbros in the showing area, and Crestaurum andesties and metagabbros north of Vee Lake. Drilling has tested the west zone shear along most of the 1km between Gold and Vee Lakes to an unknown depth. It comprises chlorite +/- sericite schist. Mineralized lenses within this part of the shear are small, and comprise lenses and veins of quartz +/- carbonate, mineralized with pyrite +/-arsenopyrite and gold. The gold occurs with the sulphides or as free gold. Good grades have been encountered over narrow widths (Knutsen 1974). The zone has also been drill-tested beneath Vee Lake (by different operators, working the PRW claims) with negative results (NMI Au 10 and AR 061044).  In 1977 the west zone was judged to have a small open pit potential (NMI Au 08)."
085JNE0051,169,1,"The Big Hill West dyke swarm, also known as the BA or Murph, occurs in the Yellowknife metasedimentary basin within the Slave structural province. It is a member of the Yellowknife pegmatite field, a series of pegmatites east of Yellowknife, NWT that are probably associated with a number of late Archean granitoid intrusions of the Prosperous Granite suite.  The pegmatites tend to occur in Burwash Formation sediments where those have been metamorphosed to lower amphibolite facies. The pegmatites show a broad zonation around the larger intrusives in the area; an inner zone dominated by Be-rich pegmatites is successively enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-rich varieties.  The Big Hill West pegmatites are Li-rich varieties that occur in a northeasterly trending dyke swarm, cutting the trend of bedding in the host metasediments at a low angle. The swarm has a strike length of 1280 metres and a width of about 150 metres. It consists of four main subparallel dykes which are each up to 20 metres wide. The pegmatites are classified as simple rather than zoned, since crystals are generally a few centimetres across and the various minerals are distributed relatively evenly throughout.  Minerals present, listed in order of abundance, are: microcline, spodumene, quartz and muscovite. A secondary, fine grained plagioclase-muscovite alteration is common, constituting as much as 50% of the dykes in places. It has affected spodumene and greatly reduced its abundance in places. The alteration is particularly common where dykes finger out. Although most of the dykes contain abundant spodumene (up to 30% by volume), some contain less than 5%.  "
085JNE0051,170,2,"Reserves are estimated (AR 080273) at 1.3 million tons grading 2% Li2O although the writer felt that the number of samples taken was too low to justify this grade figure. He noted, however, that drilling in the 1950s (AR 082348) proved that the dykes continued to at least a depth of 150 metres. In 1979, Canadian Superior returned to excavate 13 new trenches. No new reserve figure was estimated (AR 080957). Lasmanis (1978) estimates 7,888,000 tons of rock grading 1.47% Li2O under the property, which includes the Big North and Big Hill East deposits."
085JSE0050,171,1,"The showing occurs in the Western Plutonic Complex where the plutonic rocks invade the western edge of the Yellowknife Volcanic Belt. This belt is a north trending, steeply dipping sequence of Archean Yellowknife Supergroup volcanics and minor sediments. The Complex along its western margin comprises felsic intrusions of at least five ages, each mappable in a distinct terrane, forming a body of batholithic proportions ranging from gabbro-tonalite to trondhjemite-granodiorite-granite in composition. The Belt and the Complex are cut by Proterozoic diabase dykes of two or three generations. Regional metamorphism in the Belt achieved lower amphibolite grade adjacent to the Plutonic Complex. Regional, high-angle, reverse shear zones within the Belt locally host significant gold deposits (eg. Giant Mine, Con Mine) but do not cut the Complex. Later Proterozoic faults cut both the Belt and the Plutonic Complex, locally displacing their mutual contact on a regional scale.  The showing is 4.5 to 5.0 km west of Yellowknife Bay and just SW of Baker Lake, in an area underlain by massive, fine to coarse-grained, grey and pink biotite granodiorite intruded by pegmatite and aplite and locally containing volcanic inclusions. Areas of the host granite containing volcanic inclusions appear to be important to mineralization (GSC P 65-11). According to Atkinson and van Breeman's (DIANDEO 90) descriptions, the host unit must be part of the Upper Defeat Suite phase, a series of homogeneous, porphyritic, biotite trondhemite-granodiorite-granite lobes representing the late uppermost level of the Defeat Suite, and invading the Volcanic Belt at the eastern edge of the Complex. The Martin Fault, a regional Proterozoic fault, cuts NW through Baker Lake about 1 km NE of No.15 and 1.4 km NE of No.22."
085JSE0050,172,2,"Gold is hosted by various altered, quartz-filled fractures, fracture zones, and shear zones, the main ones being Veins No.15, No.22 and No.11S. The zones are generally consistent in width but do vary, from one narrow crack to a 3.5 m wide shear. The wallrock is invariably hematized, for 0.3 to 1.0 m from the zone. The main zones in the area comprise sheared quartz in pinched out lenses, stringers and pods, often ribboned with aplitic material, and surrounded by sheared granitic and aplitic rocks (GSC P 64-22).  The quartz is lightly mineralized with pyrite and hematite (less than 1% combined), and locally galena, chalcopyrite and sphalerite. Gold occurs free and associated with sulphides, and visible gold has been observed in numerous different zones on the Rodstrom property (see also J Group and C Group).  No.15 Vein is the object located by the given coordinates. It has been exposed along 55 m at NE/65E, with possible extensions 50 m NE and 45 m south. The innumerable quartz lenses comprising the Vein yielded encouraging gold values in trenches along a 24 m length in 1963 (GSC P 64-22), and drilling of 2342 m in 57 holes in 1964 defined a 33.5 m long shoot at about 7.5 m depth, which averaged 46.6 gpt Au across 1.1 m. Interest in the showing waned until it was re-staked in 1975. Reserves for No.15 were calculated in 1976 at 843 tonnes grading 49 gpt Au across 1.1 m, with additional inferred reserves of 1397 tonnes grading 28 gpt Au across 1.1 m (MIR 1976).  The No.22 Vein is about 550 m WNW of No.15. It is exposed along 37 m at 050/45 - 50dSE, and is traceable for several hundred fee, possibly more than a thousand feet (300 m)."
085JSE0050,173,3,"Surface sampling after its discovery in 1964 indicated an average grade of 93.9 gpt Au across 0.8 m for a length of the vein (GSC P 65-11); re-evaluation in 1975/76 resulted in calculated reserves of 141 tonnes at the same grade and width (MIR 1976). The No.22 Vein contains a greater proportion of chloritic volcanic inclusions at depth (GSC P 65-11).  The No.11S Vein lies between the other two, about 450 m NW of No.15. Parts of it are said to contain lenses of high-grade material (GSC P 65-11).  A 1976 test by Cominco Limited on a sample of ore grading 77.6 gpt Au (presumably from No.15) showed a 99.07% recovery using standard cyanidation techniques."
085NNE0001,174,1,"The Cab (Gar) Bi-Co-Cu-Au deposits are located in the southern Great Bear Magmatic zone, a 1.88-1.86 Ga zone of calc-alkaline, mainly intermediate, subaerial volcanic and plutonic rocks within the Wopmay orogen. Mineralization occurs in a northwesterly trending belt of Aphebian Snare Group sediments which are unconformably overlain by rhyolitic volcanic rocks related to the Great Bear Zone. The rhyolites and related volcaniclastic rocks are relatively undeformed and are tilted gently to moderately to the north. All stratified rocks are surrounded by granodiorite, quartz monzonite and granite intrusives of the Great Bear Zone. Snare Group rocks are metamorphosed to greenschist facies.  Bi-Co-Cu-Au mineralization is hosted within metasediments of the Snare Group which strike northwest and dip steeply to the northeast. Lithologies are broadly divided into a relatively uniform, fine grained, thinly bedded siltstone and a more variable unit of quartzite-argillite. The latter includes massive quartzite which grades into thinly bedded argillites containing variable amounts of chlorite and/or magnetite as laminae. These have been interpreted by some as oxide facies iron formations and in places grade from a magnetite-rich base up into a chlorite-biotite rock and then into argillaceous quartzite. In the deposit area, one of these horizons has been traced over a 1 km strike length and varies in thickness from a few centimetres to 2 m. A second chlorite-rich unit higher in the section includes thinly bedded dolomite. Chlorite-rich horizons are often complexly and tightly folded.  "
085NNE0001,175,2,"All major sulphide occurrences are associated with the chlorite-rich rocks. Arsenopyrite is the predominant sulphide and occurs as  disseminations, coarse-grained aggregates of subhedral to euhedral crystals, and veins. In chlorite-rich horizons, it forms thin layers and lenses parallel to bedding while in more competent quartzite it tends to occur in cross-cutting veins or fracture zones. Where chlorite-rich rocks are strongly folded, it may occur as cross-cutting veinlets. Disseminations occur in both rock types. Pyrite and chalcopyrite occur as coarse aggregates with arsenopyrite in places. Bismuth minerals, including mainly bismuthinite, native Bi and emplectite, are present in small grains, either interstitially in arsenopyrite aggregates or within arsenopyrite crystals. Cobalt is present mainly within the arsenopyrite lattice and to a much lesser extent as small grains of cobaltite.  Many of the occurrences are cut by feldspar porphyry dykes and arsenopyrite appears to have been remobilized into fractures within the dykes as well as into massive podiform accumulations within layered rocks near the dyke margins. The maximum strike length of any of the showings is on the order of 100 m and some reach a maximum width of about 10 m. Many consist of several sub-parallel zones.  New Athona Mines Ltd. outlined two main zones of mineralization with trenching and drilling in the late 1960's. Based on this work, they reported a reserve of 194,700 tonnes grading 0.162% Bi and unspecified levels of Cu, Co and Au in the No. 1 zone.  The No. 2 zone is a 3 m wide zone of massive arsenopyrite with very short strike length from which individual samples returned values of up to 0.21 opt Au, 0.66% Bi and 3.28% Co."
085NNE0035,176,1,"Sue (commonly known as Sue-Dianne) is an Olympic Dam-type mineralization containing copper, uranium, gold, silver and iron concentrations.  Ore minerals occuring on the showing include chalcopyrite, bornite, chalcocite and pitchblende.  The deposit occurs in a pipe-like, magnetite cemented, brecciated horizon comformable with a package of thick ash flows.  These rocks are situated on the eastern side of the Bear Structural Province (Proterzoic aged rocks) within the Great Bear Magmatic Zone.  The property operated through a joint venture between Fortune Minerals NWT and Noranda Inc. (GNWT RWED, MOG Book (1997))."
085NNE0045,177,1,"The Lou Lake showing is a gold, bismuth, cobalt, copper and tungsten oxide showing  occurring within 4 kilometres south-southeast of Lou Lake.  The showing, comprise of three closely spaced mineralized zones (Summit Peak, Bowl and Nico Lake),  occur in 1 to 65 metre stacked lens of black rock schists and breccias with variable mineralization.  These lens are stratabound and strike southeast for approximately 900 metres (GNWT RWED, MOG Book (1997))."
085NSE0043,178,1,"The Camp Lake gold showing consists of auriferous lenticular zones containing sulphide bearing (pyrite, pyrrhotite, arsenopyrite, sphalerite, galena and chalcopyrite) in stringers within shear zones which are conformable with greywackes of the Archean Yellowknife Supergroup. Diamond drill indicated resources of 51,150 tons at 0.40 oz/t OR 13,050 tons at 0.35 oz/t gold are listed.  This showing has been subjected to intermittant exploration from 1938 to 1981. Work included: surface exploration, sampling, diamond drilling and a feasibility study (1981)."
085NSE0044,179,1,"The Slemon showing is underlain by Archean Yellowknife Supergroup sediments and intrusive quartz porphyry sills which contain gold bearing quartz veins, stockworks and breccia zones. The latter contain gold bearing bands of massive pyrite plus some silver and bismuth tellerides. Possible mineral resources are listed at 35.000 tons at 0.2 oz/t gold OR 60,000 tons at 0.4 oz/t gold using diamond drill sludge samples.  This showing has been subjected to sporatic exploration from 1939 to 1987. Work included trenching, diamond drilling, test pitting, soil sampling, mapping, pitting and bulk sampling."
085OSE0007,180,1,"Regional The region is predominantly underlain by massive greywackes and minor argillites of the Archean Yellowknife Supergroup which strike NNE and dip nearly vertically. A band of mafic to intermediate volcanics several hundred meters wide, extends along the east side of Goodwin Lake, while chloritic tuffs, mixed with greywackes occur near Barker Lake. Coarse grits to pebble conglomerate were observed locally. Bedding tops generally point to the west.  Conformable with the stratigraphy are a number of medium grained quartz diorite sills. Contacts are often not too sharp because of the fine grained chill margin and alteration of the enclosing sediments. Many showings are located in proximal to these sills. An erratic distribution of diabase dykes occur on the property as a late stage post mineralization event.  Two stages of deformation have affected the stratigraphic sequence, resulting in tight isoclinal folds with very steep plunges and long limbs that are nearly vertical. Usually only minor flexures such as small drag folds and minor strike slip faults are observed near the fold noses.   Metamorphism is of the lower greenschist facies."
085OSE0007,181,2,"Property The claims are underlain by sedimentary rocks which are a series of interbedded, fine-to-medium grained greywackes and argillites of the Yellowknife Supergroup which strike NNE and dip nearly vertical. A band of mafic to intermediate volcanics several hundred meters wide extends along the east side of Goodwin Lake, while chloritic tuffs mixed with greywackes occur near Barker Lake. Coarse grits to pebble conglomerate were observed locally. Bedding tops generally point to the west.  Conformable with the stratigraphy are a number of medium grained quartz diorite sills. Contacts are often not too sharp because of the fine grained chill margin and alteration of the enclosing sediments. Many of the showings are located in proximity to these sills. An erratic distribution of diabase dykes occur on the property as a late stage post mineralization event.  The host of the deposit is a quartz diorite sill which intrudes these sedimentary rocks. The sill outcrops at intervals for a length of 2,400 feet and varies from 15 to 60 feet in width. It strikes nearly north 35 degrees east and dips about 80 degrees southeast parallel with the enclosing strata."
085OSE0007,182,3,"Showing The diorite host sill contains rounded fibrous clots of amphibole from one sixteenth to one eighth of an inch in diameter.  Minute grains and blebs of pyrrhotite occur throughout, and together with a little pyrite, comprise several percent of the rock.  Quartz bodies cut the diorite and generally do not extend into the adjacent strata. The quartz is commonly concentrated near or at the walls of the sill, particularly the northeast wall. The quartz is light and dark grey and mottled, and adheres firmly to the wall rock. It occurs as veins and irregular masses ranging from an inch to several feet in width.  Metallic minerals, comprising less than one percent of the vein matter, are mainly arsenopyrite, pyrite, and pyrrhotite: others noted are galena, chalcopyrite, and sphalerite. Gold is reported in the quartz and in the adjacent diorite. Both the quartz bodies and enclosing quartz diorite are cut by rare veinlets of drusy white calcite and possibly pyrite."
085OSE0007,183,4,"Exploration The main zone was trenched and was tested by 13,600 feet of diamond drilling. In 1947 a shaft was sunk to a depth of 160 feet. It is inclined at 65 degrees in the direction N 35 degrees E. Underground development was done on the 150 foot level and the mined material was sent to Yellowknife for assay. Some diamond drilling was done underground. No results from trenching or diamond drilling could be located. The economic potential for this showing was calculated at 700 tons per vertical foot at a gold grade of 0.60 oz/ton. "
085OSW0001,184,1,"Regional  This Showing is in the Russell Lake - Slemon Lake Supracrustal belt. These rocks are part of the Archean Slave Province. Supracrustal rocks include minor amounts of mafic and felsic metavolcanics and abundant greywacke-mudstone metasediments, which represent a turbidite sequence similar to that found elsewhere in the Slave Province. The metasedimentary succession at Russell and Slemon lakes is characterized by abundant oxide and silicate amphibolitic iron formation that is locally sulphide rich (pyrite, pyrrhotite and arsenopyrite) and auriferous.  The supracrustal rocks have undergone at least three phases of folding, with F1 and F2 isoclines refolded about more open F3 folds. Three foliation subsets post-date F2 isoclines. Two major sets of post-Archean faults transect the area: N-NW trending sinistral faults and easterly trending dextral faults. Quartz and quartz-carbonate veins were injected througout the deformational history of the area.  Metamorphic grade ranges from greenschist to amphibolite facies. Within the metasedimentary rocks this transition is marked by a regional cordierite isograd. The isograd parallels the contact between the supracrustal rocks and the bounding granitic rocks and is offset by post-Archean faults. (MIR 1986-87)"
085OSW0001,185,2,"Property/Showing  A thick mafic intrusion cuts metasediments north of the Bugow deposits. All stratified rocks have been metamorphosed to at least upper greenschist facies and in the area of the deposits, to lower amphibolite facies. Structure in the area of the deposits is complex, recording at least two periods of folding.  The Bugow iron formation is the most significant of several iron formations situated within a sequence of turbiditic metasediments. In general, sediments underlying it are more psammitic and those above it, in which the minor iron formations are situated, are more pelitic. Intercalated with and enclosing the iron formations are black pelitic schists containing garnet, chlorite and quartz. A locally tuffaceous, intermediate to mafic volcanic unit underlies the metasediments. Numerous small pegmatites intrude both iron formation and metasediments and a large mafic intrusive has been intersected in drill core.  The iron formations are well-laminated and have been divided into a silicate facies and silicate-sulphide facies on the basis of sulphide content. Both are characterized by alternating laminae of chert and various proportions of grunerite/hornblende, garnet, chlorite, and sulphides together with minor iron oxide and carbonate. Silicate-sulphide iron formation is also distinguished by a larger proportion of cross-cutting quartz veins, an increase in hornblende at the expense of grunerite, more siliceous character and the presence of significant quantities of gold.  Sulphide minerals include, in decreasing order of abundance, pyrite, pyrrhotite, chalcopyrite, arsenopyrite, loellingite and sphalerite. Arsenopyrite is rare in contrast"
085OSW0001,186,3,"with other iron formation-hosted gold deposits in the Slave Province.  Significant levels of gold are present in a number of discrete zones in the Bugow iron formation, including the Cabin Lake, Andrew South, Andrew North, Camp, Beaver and Twilight zones. All zones are located along fold limbs despite higher levels of sulphides in fold noses. Gold occurs in association with sulphides although in detail, it is not found within sulphide grains. It is most common as 10-20 micron grains interstitial to silicates and at the boundary between quartz veins and chlorite-hornblende-rich iron formation. Less common sites include fractures near quartz veins and as inclusions in rare arsenopyrite and in pyrite.  The Cabin Lake zone has received the most exploration attention to date. Erratic, high grade drill intersections are concentrated in an area about 100 m long, 60 m deep and 12 m wide. Although the zone is stratabound, it transgresses the Bugow iron formation internally, crossing from a location near the base of the unit to one near the top. A reserve of 70,000 tonnes grading 10.29 g/t Au is reported in DIAND Mineral Industry Report 1986-87. Aber Resources' 1987 Annual Report states a figure of 100,000 tons grading 0.3 oz/ton Au."
085OSW0001,187,4,"The Andrew zones are reported to contain 43,900 tonnes grading 4.46 g/t Au (Bugow or Andrew South) and 18,100 tonnes grading 7.89 g/t Au (Andrew North, #085OSW0040) (Canadian Deposits Not Being Mined 1989).  The Bugow Showing ( Andrew South) has two satellite showings. One to the north is the Andrew North Showing (NORMIN Showing Number 085OSW0040) and the other to the south is the AH 205 (# 085OSW0041). Both of these showings are within the same iron formation unit that hosts the Bugow Showing.  North of the Cabin Lake Showing and along strike are, from south to north, the Beaver Showing (085OSW0043), the Camp Showing (085OSW0044) and the Camp North Showing (085OSW0045). All of these showings are within the same iron formation unit that hosts the Cabin Lake Showing."
085OSW0001,188,5,"The Bugow claim group has had trenching, sampling, detailed mapping, diamond drilling of the key showings and both ground and airborne geophysics. The ground and airborne geophysics done include magnetetometer, electromagnetics and induced polarization."
085OSW0013,189,1,"Regional The area is within the Slave Structural Province and lies near the south end of the Russell Lake-Slemon Lake Supracrustal belt. This supracrustal belt comprises Archean metavolcanics and metasediments of the Yellowknife Supergroup.  The Russell Lake area is largely underlain by greywacke-mudstone metaturbidites and lesser amounts of felsic and mafic metavolcanics. Felsic metavolcanics are exposed along the eastern shore of Russell Lake in a southwest trending belt. Mafic metavolcanics occur five kilometres west of Russell Lake in two narrow southwest trending belts and as a narrow southwest trending belt at Mosher Lake, some 10 kilometres east of Russell Lake. Later Archean granitoid intrussions cut the supracrustal sequences. These consist of tonalitic to granitic plutons to the northwest, northeast and south. Numerous small granitic plugs are exposed throughout the Russell Lake area.  The strike of the metasediments is generally northeast with some wrapping of the metasediments around a granitic plug near Murkey Bay on Russell Lake. The metasediments are isoclinally folded about northeast trending anticlinal and synclinal axes with preferential overturning to the west. The fine grained metasedimentary unit which hosts silicate and minor sulphide facies iron formation is repeated across Russell Lake between the metavolcanic rocks to the east and west."
085OSW0013,190,2,"Property The property is underlain by a narrow belt of volcanic rocks of the Yellowknife Supergroup that strike N-NE through Mosher Lake. On both sides greywacke and slate rocks bound the volcanics which are light to dark green andesite and basalts and massive schistose and pillowed flows. At the contacts they are interbedded with white-weathering porphyritic rhyolite and schistose tuff, agglomerate and breccia.  The slightly altered sedimentary rocks are interbedded slates, arkoses, quartzites and phyllites. The greywackes are dark grey and sandy textured and weather to a dark grey, greenish or buff colour. The sediments lie in a series of tight isoclinal folds with steep dipping or overturned axial planes. The volcanics also dip steeply but the folds seem to be broader.  Showing The showing strikes northeasterly and lies between schistose and massive basic flows in a rusty mineralized zone. The zone can be traced for 1,200 feet and carries massive, fine-grained, schistose amphibolite mineralized with pyrrhotite, pyrite, and arsenopyrite. Quartz stringers parallel the schistosity in irregular lenses and veins and also crosscut in gash veins.  The south end of the mineralized zone is terminated by tourmaline pegmatites. A fault, filled by diabase, offsets the centre of the zone 50 feet."
085OSW0013,191,3,"The gold assays from trenching on the north section returned values from trace to 0.49 oz/ton over 6 feet. Diamond drilling returned gold assays from trace to 0.70 oz/ton over 5 feet. The zone averages 0.15 oz/ton gold over 25 feet for 300 feet based on surface trenching. The zone averages 0.07 oz/ton across 58 feet based on diamond drilling for the full strike length of 1200 feet.  Drill indicated reserves to a depth of 170 feet is 552,000 tons grading 0.082 oz/ton gold.  Exploration This showing has had trenching and diamond drilling done. A resource has been calculated based on this information. Drill indicated reserves to a depth of 170 feet is 552,000 tons grading 0.082 oz/ton gold."
085OSW0042,192,1,"Regional The area is within the Slave Structural Province and lies near the south end of the Russell Lake-Slemon Lake Supracrustal belt. This supracrustal belt comprises Archean metavolcanics and metasediments of the Yellowknife Supergroup.  The Russell Lake area is largely underlain by greywacke-mudstone metaturbidites and lesser amounts of felsic and mafic metavolcanics. Felsic metavolcanics are exposed along the eastern shore of Russell Lake in a southwest trending belt. Mafic metavolcanics occur five kilometres west of Russell Lake in two narrow southwest trending belts and as a narrow southwest trending belt at Mosher Lake, some 10 kilometres east of Russell Lake. Later Archean granitoid intrusions cut the supracrustal sequences. These consist of tonalitic to granitic plutons to the northwest, northeast and south. Numerous small granitic plugs are exposed throughout the Russell Lake area.  The strike of the metasediments is generally northeast with some wrapping of the metasediments around a granitic plug near Murkey Bay on Russell Lake. The metasediments are isoclinally folded about northeast trending anticlinal and synclinal axes with preferential overturning to the west. The fine grained metasedimentary unit which hosts silicate and minor sulphide facies iron formation is repeated across Russell Lake between the metavolcanic rocks to the east and west."
085OSW0042,193,2,"Property/Showing Significant levels of gold are present in a number of discrete zones in the Bugow iron formation, including the Cabin Lake, Andrew South, Andrew North, Camp, Beaver and Twilight zones. All zones are located along fold limbs despite higher levels of sulphides in fold noses. Gold occurs in association with sulphides although in detail, it is not found within sulphide grains. It is most common as 10-20 micron grains interstitial to silicates and at the boundary between quartz veins and chlorite-hornblende-rich iron formation. Less common sites include fractures near quartz veins and as inclusions in rare arsenopyrite and in pyrite.  The Cabin Lake zone has received the most exploration attention to date. Erratic, high grade drill intersections are concentrated in an area about 100 m long, 60 m deep and 12 m wide. Although the zone is stratabound, it transgresses the Bugow iron formation internally, crossing from a location near the base of the unit to one near the top. A reserve of 70,000 tonnes grading 10.29 g Au/t is reported in DIAND Mineral Industry Report 1986-87. Aber Resources' 1987 Annual Report states a figure of 100,000 tons grading 0.3 oz/ton Au.  An Aber Resources Ltd. press release dated 1986/08/18 summarizes the assay results from the first four diamond drill holes from the Cabin Zone. Hole A86-1 averaged 0.35 oz/ton Au across 29 feet, hole A86-2 averaged 0.24 oz/ton Au across 16 feet, hole A86-3 averaged 0.46 oz/ton Au across 26.3 feet and A86-4 averaged 0.23 oz/ton Au across 5.0 feet, 0.20 oz/ton Au across 10.0 feet and 0.46 oz/ton Au across 20.0 feet."
085OSW0042,194,3,"Work on the Bugow claim group includes trenching, sampling, detailed mapping, diamond drilling of the key showings and both ground and airborne geophysics. The ground and airborne geophysics done include magnetometer, electromagnetics and induced polarization."
085PSW0001,195,1,"The Nicholas Lake vein gold deposit is located near the northern end of the Yellowknife Basin, a supracrustal belt within the Archean Slave structural province. Turbiditic metasediments of the Burwash Formation, part of the Yellowknife Supergroup, have been intruded by pink granite and a medium to coarse-grained granodiorite which is the host for mineralization. Numerous dykes and irregular masses of granodiorite are present in an area extending southwest of the main granodiorite intrusion. The metasediments have been deformed into tight folds with bedding now generally striking northwesterly with a steep dip. A strong, parallel to subparallel axial plane foliation is superimposed on the stratified rocks. Regional metamorphic grade is lower amphibolite facies.  The Nicholas Lake deposit comprises a series of essentially vertical quartz-sulphide veins in a subvertical to vertical, altered granodiorite stock about 200 m in diameter intruding metasediments. Intense shearing, sericitization and silicification are common, particularly along the southern contact. At least three varieties of quartz have been recognized and multiple episodes of brecciation and rehealing are evident. The best veins and gold values are concentrated along the southern altered border zone and are restricted to the granodiorite.  Higher grade gold values are associated with massive, fine-grained pyrrhotite coating angular fragments of arsenopyrite and quartz, massive arsenopyrite and pyrite with lesser sphalerite and galena, vein quartz with visible gold and coarse-grained sphalerite and galena, and quartz veins with pyrite. Some gold is present in association with disseminated sphalerite and minor quartz veinlets within zones of brecciated and fractured granodiorite."
085PSW0001,196,2,"Sulphides may also occur as massive lenses up to 65 cm wide.  The deposit has been traced by drilling over a strike length of 200 m and to a depth of about 300 m. A reserve (indicated and inferred) of 1,114,600  tonnes grading 12.16 g Au/t has been calculated using a cutoff grade of 5.0 g Au/t. Metallurgical tests established that 94% of the gold could be recovered using a 60% minus 200 mesh grind and flotation of sulphides followed by a regrind to 90% minus 350 mesh and cyanidization."
085PSW0035,197,1,"Gold mineralization occurs in short, narrow quartz veins cutting fragmented Archean amphibole gneiss of the Yellowknife Supergroup. Diamond drill intersected gold bearing veins at 400 and 800 feet gave a reported average grade of 0.3 oz/t in the main zone. A resource of 100,000 tons at 0.62 oz/t is listed.  Sporatic exploration was done from 1944-56 and included trenching, geological mapping, sampling and diamond drilling. In 1981 Newmont Exploration Canada optioned the property and subjected the showing to geological mapping, sampling, geophysical surveys of magnetics, EM, IP and diamond drilling."
085PSW0037,198,1,"In the Cross Lake showing visible gold is associated with sulphides in quartz veins within a shear zone cutting a knotted quartz mica schist derived from impure greywacke and slate of the Archean Yellowknife Supergroup.  A diamond drill indicated resource was listed 30,000 tons at 0.31 oz/t"
085PSW0040,199,1,"Visible gold in discontinuous quartz veins in greywacke of the Archean Yellowknife Supergroup. This showing has been subjected to sporatic exploration since the 1940s including, pitting, trenching and diamond drilling. A diamond drill indicated resouerce of 4,400 tons at 0.47 oz/t is listed."
086BSW0002,200,1,"The Kim prospect (Main Zone) is located in the Indin Lake supracrustal belt, part of the Archean Slave structural province. The belt consists of irregular, generally north-trending belts of Archean Yellowknife Supergroup rocks, including mainly basaltic volcanic rocks, turbiditic greywackes and mudstones dated at 2669 +/- 15 Ma. Intervening areas are made up of hybrid rocks derived from both basement granitoid and supracrustal rocks as well as plutonic rocks, generally granite or granodiorite.  Detailed mapping by Echo Bay Mines has identified the following stratigraphy in the area of the deposit: a basal sequence of pillowed and massive basalts and irregular gabbroic bodies overlain by the lower massive basalt, a lower amygdaloidal pillow unit characterised by carbonate amygdules, an upper massive basalt and finally an upper amygdaloidal pillow unit characterised by quartz-feldspar amygdules. The volcanic package has been metamorphosed to amphibolite facies, but is in fault contact with a package of turbidites which are at lower greenschist facies. This vertical ductile fault represents a major break in the area, which is structurally complex. Sedimentary rocks are isoclinally folded and broader folding is recognised within the volcanics. Northwest-trending left-lateral strike-slip faults with near vertical dips, are the latest and predominant faults in the area.  The Main Zone on Lex Lake is a stratabound deposit, consisting of quartz-carbonate veins in fractured, sulphide-rich, silicified massive basalt flows about 60 metres from their contact with the sediments. It strikes northerly and dips steeply to the west. An early white quartz vein set is cut by a later smoky quartz-carbonate set with which the gold is associated."
086BSW0002,201,2,"Veins are deformed and show strong ribbon textures along their contacts. Both arsenopyrite and pyrrhotite are found within the veins and in haloes extending 20 to 30 cm from them. Pyrrhotite crystals are aligned along a prominent and steeply plunging stretching lineation commonly developed in basalts in the immediate area of the deposit. Arsenopyrite is generally massive to euhedral, overgrows and possibly replaces pyrrhotite and is commonly brittley deformed along the stretching lineation. Free gold, in places visible, is found in quartz-carbonate veins, in fractures cutting arsenopyrite crystals and in sulphide-rich haloes adjacent to veins.  Total drilling on the Main zone in the period 1984-1990 was 13,607.5 metres. Mineralization has been intersected over a strike length of 731 metres and has an average width of 4.6 metres. The zone has been divided by faulting into six blocks. In 1987, a reserve totalling 112,500 tonnes grading 7.89 g Au/t was calculated for one block containing about 10% of the total tonnage. The cutoff grade used was 4.00 g Au/t and minimum width 1.5 metres. Four deep drill holes have confirmed the depth extension of mineralization to 365 metres and the deposit remains open at depth. A three tonne bulk surface sample was collected for metallurgical and conductivity sorting tests."
086BSW0003,202,1,"The Cass prospect is located in the Indin Lake supracrustal belt, within the Archean Slave structural province. The belt consists of irregular, generally north-trending belts of Archean Yellowknife Supergroup rocks, including mainly basaltic volcanic rocks, turbiditic greywackes and mudstones dated at 2669 +/- 15 Ma. Intervening areas are made up of hybrid rocks derived from both basement granitoid and supracrustal rocks as well as plutonic rocks, generally granite or granodiorite.  The Cass zone is located about 3 km southwest of the Main zone constituting the Kim prospect. Gold occurs in steeply dipping quartz-carbonate veins cutting and restricted to a northeast-trending, subvolcanic gabbroic sill which intrudes a sequence of intermediate to felsic flows and pyroclastics. The gabbro varies in width from 20 to 100 m and has a strike length of approximately 2 km.  Mineralization is associated with two sets of smoky-white, mottled  quartz and quartz-carbonate veins up to several metres long and up to 0.5 m wide. The less abundant quartz-rich set is sub-parallel to regional foliation while the quartz-carbonate set cuts it at 70-80 degrees and is oriented at a high angle relative to the gabbro contacts. Several layers of carbonate and quartz are present in each vein, with carbonate tending to occur in the central portions. The veins are folded about steeply plunging axes, both in a gross sense involving the entire vein and internally. Grunerite-garnet veins with diffuse contacts extend outward from the quartz-carbonate veins and form selvages around them. Garnet is also present in haloes around the veins."
086BSW0003,203,2,"Arsenopyrite occurs in diffuse zones of coarse-grained euhedral crystals adjacent to veins in the silicified metagabbro and as anhedral crystal masses within the veins and along vein contacts. Pyrrhotite is most abundant in haloes 30 - 50 cm wide adjacent to veins but is also disseminated throughout the sill. Pyrite is found as cubes and irregular aggregates. Gold occurs within sulphides and as native metal concentrated along the contacts of the quartz-carbonate veins. Both arsenopyrite and pyrrhotite have been deformed, the former fractured and brittly boudinaged along a regional lineation, the latter elongated parallel to it.  Drilling in the period between 1984 and 1990 totalled 10,479 m. The Cass zone has been traced by drilling over a strike length of 300 m, to a depth of 210 m and is open to the southwest. It ranges between 1 and 15 m in thickness, averaging 4.9 m. A probable reserve on a 120 m long by 210 m deep block has been calculated at 336,300 tonnes grading 7.17 g Au/t. A three tonne bulk surface sample was collected for metallurgical and conductivity sorting tests."
086BSW0019,204,1,"Mineralization withion a series of conformable auriferous quartz veins, stringers and lenses hosted by by N-NNE striking greywackes, slates and volcanics of the Archean Yellowknife Supergroup. The No. 1 vein mineralogy consists of quartz-pyrite-arsenopyrite, pyrrhotite, chalcopyrite and visible gold. A resource of 29,000 tons at 0.35 oz/t has been calculated.  Work on the showing includes trenching, diamond drilling, geochemical sampling and  geological mapping."
086BSW0027,205,1,"Galena, sphalerite, arsenoipyrite, chalcopyrite and gold mineralization occurs in a 100 foot wide belt of argillite-quartz veining in siltstone-shale unit within the Proterozoic Snare Group. A 5x8 foot wide mineralized zone plunges 45 degrees below the lake to a depth of 300 feet below the lake. Exploration on this showing include trenching, geological mapping and sampling, diamond drilling, EM geophysical surveys and a petrographic study. A diamond drill inferred resource of 81,000 T at 0.228 oz/t gold (uncut) is listed."
086BSW0028,206,1,"In this showing gold is found in sediments of the Yellowknife Supergroup at or near the conbtact with volcanics. Aurioferous zones are generally silicified, probably due to the intrusion of the 6-12 m wide Gamble Dyke, an albite-porphyritic ENE trending dyke. Work done on the showing includes trenching, geological sampling, diamond drilling, geological mapping, soil sampling and geophysical magnetic and EM surveys. Resources calculated are probable at 116,185 tons at 0.411 oz/t gold (diluted) plus 33,972 tons at 0.128 oz/t gold."
086BSW0029,207,1,"Zones of auriferous quartz veins and stringers are offset by NNW trending faults in schistose greywackes and argillites of the Archean Yellowknife Supergroup. Metallic minerals comprise approximately 1% of the vein material and include pyrite-arsenopyrite-pyrrhotite-galena-chalcopyrite-sphalerite and jamesonite and free gold.A resource of 72,500 tons at 0.36 oz/t gold is listed.  Work done on the showing includes: 1945-49: trenching, diamond drilling, sinking a shaft to the 525 foot level (3 levels, 1979-82: shaft rehabilitation and dewatering, 1988: diamond drilling."
086BSW0035,208,1,"Two zones, the Main and the A make up this showing. The Main zone comprises a gold bearing stockwork of quartz veinlets in aconformable graphitic shear in sediments of the Archean Yellowknife Supergroup. Outside the Main shear, gold occurrences are associated with conformable quartz veins in volcanics. A shaft was sunk to 525 feet and lateral work explored the A zone on the 175 foot level and the Main zone on the 300 foot level.  Resources calculated: A zone = 23,000 tons diamond drill indicated at 0.54 oz/t (1948); Main zone = 600x5 at 0.44 oz/t gold to depths of 160 feet to 300 feet. A 1980 reevaluation of unspecified North Inca deposit(s) produced an estimate of 90,000 tons at 0.20 oz/t gold."
086BSW0050,209,1,"The Indin Lake area is situated in the southwestern portion of the Slave Structural Province near the contact with the Bear Structural Province (Wopmay Oregon).  It is underlain by Archean age rocks which are part of the Yellowknife Supergroup and are comprised of volcanic and sedimentary strata forming a north-northeast trending supracrustal belt. This irregular shaped belt extends south approximately from the south side of Truce Lake to the southern portion of the Snare River.  The Indin Lake Supracrustal Belt is bounded to the west by Archean granitoid plutons and migmatites while gneissic rocks flank the eastern side and are thought to be basement rocks to the belt.  All the rocks within the belt are strongly folded and there is a  complicated deformation history associated with the area.    Volcanic rocks of the Indin Lake area occur as mafic, intermediate and felsic units.  Mafic lithologies dominate the volcanic suite of rocks, which include pillowed flows (minor andesite) and local interflow breccias. Intermediate rocks include volcaniclastic units (mainly breccias) occurring usually as lens shaped bodies and may dominate the lithology within small isolated portions of the belt (eg. Leta Arm and Spanner Lake areas) .  Ocurrences of quartz diorite and gabbro sills, scattered throughout the Indin Lake Belt, are thought to be related to the volcanic units in the area .  One of these sills adjacent to Baton Lake is an albitic and auriferous intrusive within a mafic volcanic package and hosts the Colomac Mine deposit (showing I.D. No. 086BSW0004 and reference I.D. No. 1994-Cp91)."
086BSW0050,210,2,"Sediments in the area comprises turbiditic greywackes and mudstones.  Hosted within the sediments in the eastern portion of the Indin Lake Belt are strongly folded banded iron formation units consisting of  five main facies: silicate-oxide facies, silicate-amphibolite facies, silicate-sulphide facies, silicate-chlorite facies and cherty exhalitive facies.  These iron formation units occur as lens/pods or conformable beds that may be traced out for several kilometres with widths up to 10s of metres and are locally auriferous.  Quartz veins (locally auriferous) often cut the exhalitive and turbiditic units, with increased concentrations in the area of the fold noses (reference I.D. No. 1994-Cp91 and 083396).  Granodiorites and pegmatites intrude the belt and generally cut the volcanic and turbidite rocks with variable emplacement ages.  Possible synvolcanic emplacement has been obsereved locally within the area.  The Cotterrill Lake complex (hornblende - biotite granodiorite/hornblende monzogranite) is basement rock within the belt.  Diabase (to gabbro) dyke swarms occur throughout the Indin Lake area and cut all pre-existing rock units.   Evidence of four deformational events was observed by Pehrsson and Beaumont-Smith (reference I.D. No. 1994-Cp91) while preforming mapping in the Indin Lake Supracrustal Belt.  All the rocks in the belt have been metamorphosed to lower greenschist to amphibolitic facies.   "
086BSW0050,211,3,"The Horseshoe Zone is described as a banded iron formation hosted within a greywacke-argillite package all of Archean age.  The zone is situated within a synclinal fold structure with the main mineralization occuring at the closure, extending into the limbs of the fold.  Drilling has indicated that gold is concentrated in layers through the iron formation.  A strike length of at least 1,000 feet has been intersected during the exploration surface drilling.  Information on the showing is available only from news releases where only limited details are given."
086BSW0050,212,4,"The Horseshoe Zone is located along the southern shore of Damoti Lake and is associated with several other banded iron formation gold showings in the vicinity.  The Horseshoe Zone has two other smaller zones (Pyrite Zone and Red Mountain Zone) directly adjacent to it and can be considered all part of one zone.  The zone was first discovered in a 1993 exploration programme which included bedrock sampling and mapping at a 1:2000 scale, over the southern portion of the Damoti Lake property.  One grab sample described as a medium grained amphibolite with thin pyrite stringers assayed 1.41 g/t gold. Additional work (1994 to 1998) included surface exploration drilling and an underground decline into the zone in order to better delineate the mineralization.  Mineralized iron formation (4000 tons) was mined from 2 exploration drifts and stocked piled for future processing.  A  few underground exploration diamond drill holes were completed to aide in delineating the extent of gold mineralization.  More than 35 surface diamond drill holes have been drilled into the Horseshoe Zone todate with very significant results including 12.143 feet at 4.380 oz/ton gold (D94-113) and 10.50 feet of 0.680 oz/ton gold (D97-307).  Reserve calculations were completed on the zone resulting in a demonstrated reserve figure of 212,350 ounces of gold  and an inferred resource of 148,178 ounces of gold. "
086DNE0002,213,1,"Numerous occurrences, generally high grade pitchblende pods of restricted spatial extent. Numerous of these have been examined by drilling, open pits, or underground work including drifting and raising. No. 3 and No. 4 as sampled underground on three consecutive raise faces yielded an average of 0.678% U3O8 across 3.88 ft for a raise length of 16 ft. A combined 1.5 tons of ore  assaying 40.5% U3O8, taken mostly from pits on No. 3 and No. 4, is said to have basically cleaned out those two showings; however, two lenses in the No. 3 and No. 4 area are also said to contain an estimated 200 tons grading 3% U3O8. 1970s drilling could find no extensions to these lenses."
086DNE0004,214,1,Undg dvlp outlined ore zone of 300 by 1.5 ft with 0.35% U3O8.
086HNE0087,215,1,"The Izok Lake deposit lies within the Point Lake Volcanic Belt, a north trending belt of Archean mafic to felsic volcanics and subordinate sediments which have been subjected to polyphase Archean deformation and regional metamorphism. The deposit is beneath Izok Lake, in the Izok sub-belt, a NE to north trending arm of volcanic supracrustals which juts from the east side of the Point Lake Belt just north of Itchen Lake. The rocks in these belts belong to the Point Lake Formation of the Yellowknife Supergroup.  Itchen and Contwoyto Formation metaturbidites, also of the Yellowknife Supergroup, overlie the Point Lake Fm and are exposed about 2 km SE of Izok. 2 km SW of Izok, a sedimentary-felsic volcanic sequence is now exposed as siliceous gneisses. Within a kilometre north and east of Izok, a mixed sedimentary-volcanic sequence correlative with Yellowknife Supergroup rocks, is intruded by numerous, late Archean granitic sheets, creating lit-par-lit gneisses. The granitic bodies coalesce into the Rockinghorse Batholith about 2 km NE of Izok.  The deposit is hosted near the top of a thick felsic pile, by rhyolitic and dacitic flows and tuffs metamorphosed to felsic gneisses. It is conformably underlain by similar rocks, and toward the edges of the Central Zone is underlain by rhyolite agglomerate. It is conformably overlain by felsic flows and tuffs, and near the felsic centre by a pyritic muscovite schist, perhaps derived from a cherty tuff. Minor mafic gneisses in the hangingwall are probably derived from intermediate to mafic tuffs. An amphibolite unconformably overlies the host felsic volcanics, and three bodies of amphibolitic metagabbro intrusive into the volcanics outcrop around Izok Lake."
086HNE0087,216,2,"Massive to pillowed, mafic to intermediate flows overlie the felsic pile. A late Archean, tourmaline granite-pegmatite cutting the deposit is locally Pb-enriched.  The deposit consists of the North and Central Zones, initially described separately but recently discussed as one; the Northwest Zone; and the recently discovered Inukshuk Zone. The Central-North Zones form a trough-shaped, flat-lying, composite lens of massive sulphides measuring 450 by 110 m horizontally. Its long axis trends ENE and plunges 15-30 degrees ENE. It has a highly variable thickness, from 0 - 160 m deep. A Cu-rich stringer zone under the west end of the Central Zone is south dipping, about 100 m long x 20 m deep, at a depth of 100 - 160 m from surface.  The Northwest Zone, centred about 250 m NW of the Central Zone, is a fairly flat-lying lens, somewhat concave upwards and dipping shallowly north. Its surface lies at 30 - 130 m depth and it measures 200 by 280 m horizontally and 22 m vertically. Both the Central and the Northwest Zones are open-pit prospects with a stripping ratio of 3:1. The Inukshuk Zone, discovered in 1992 400 m east of the main deposit, is an elongate, ENE-trending lens dipping shallowly south. It measures greater than 300 m long by 150 m by 10 m thick, at 60 - 400 m depths. It partly underlies Izok Lake and, unlike the main deposit, is an underground mining prospect.  The main deposit (Central and Northwest Zones) lies in NE-trending and plunging, synclinal folds. The variable thicknesses of the sulphide layers is interpreted to be partly an original depositional feature, which may have localized fold axes, and partly due to deformational boudinaging and necking.  Sulphides are coarse grained and massive, comprised of mainly sphalerite, chalcopyrite, pyrite and pyrrhotite."
086HNE0087,217,3,"Zoning in the Central Zone, above the Cu-rich stringer zone, consists of a massive, Cu-rich basal section overlain by a Zn-rich section, itself locally overlain by a Zn-Pb-rich section. There is considerable evidence for re-mobilization of galena and chalcopyrite during deformation and/or metamorphism, and this apparently has disrupted more subtle zonations.  Sericite-biotite alteration is pervasive in an envelope around the deposit, silicification is less extensive and intensive, and minor aluminosilicate alteration has been noted. A Mg-enriched, chlorite- cordierite-anthophyllite rock underlies a marked thinning of the Central Zone and is interpreted to represent a conduit for upwelling hydrothermal solutions through a volcanic cone or ridge.  Reserves were estimated in 1992 at 2 million tonnes of 2% Cu and 8% Zn, inferred, for the Inukshuk Zone, open down-plunge. Also in 1992, the main deposit was estimated, on the basis of 148 DDH on 60 m centres, to have probable and possible reserves of 12.0 million tonnes grading 31.% Cu, 1.4% Pb, 14.5% Zn and 74.8 g/t Ag, and inferred reserves of 1.4 million tonnes grading 3.8% Cu, .8% Pb, 13.1% Zn and 66.5 g/t Ag."
086HSE0032,218,1,"The showing is in the Contwoyto - Itchen - Point Sedimentary Terrane, a large arcuate belt of Archean turbiditic metasediments of the Yellowknife Supergroup. It is flanked 5 km to the west by the older, predominantly volcanic Point Lake supracrustal belt, and invaded to the east by late Archean granitoids. Late Proterozoic diabase dykes cut all other lithologies.  The Contwoyto Formation sediments underlying the showing area consist of schistose argillites with subordinate greywacke and interbedded lenses and layers of iron formation. These strike N and dip 50E to vertically. A cordierite isograd marking a transition to lower amphibolite facies is immediately east of the showing.  The showing is a zone of iron formation and interbedded black, fine grained, graded-bedded argillite locally grading into greywacke. The iron formation, in 3 and locally 4 discrete members, is folded and overall N-striking and almost vertical. It a garnet-amphibole iron formation with abundant cross-cutting and conformable quartz veins, and conformable sulphide layers made up of disseminated pyrrhotite, arsenopyrite, and pyrite. The host unit has been traced by exposure and geophysical response for 700-800 m, the northernmost 490 m of which is overburden-covered. At least 100 m and probably 350 m of its strike length has been systematically drill-tested. It averages 3.5 m thick at surface but ranges between 10 and 35 m thick to depths of 300 m. Gold appears to be evenly distributed throughout and the potential exists for 2 to 3 million tons grading 0.29 oz/ton (George Cross Newsletter, 1989 No.235 & 1990 No.89 & 179)."
086ISE0001,219,1,"The Takijuq-Hood deposits lie in the northern Slave Province, in the Takijuq Lake-Hood River Supracrustal Belt, a 125 km long, NNE-trending belt of Archean Yellowknife Supergroup mafic to felsic volcanics and various intrusives into them. At its north end, the Belt is only a few kilometres south of the southern end of the Anialik River Supracrustal Belt, and its south end apparently adjoins the north end of the Point Lake Belt (EGS 1992-16). Near its south end, at the south end of Takijuq Lake, the belt widens into an ENE-trending segment 8 km long and 1.5 km wide. This Takijuq South Segment hosts the Takijuq-Hood deposits and showings.  The Segment contains a greater proportion of felsics than the rest of the belt. The felsics are under and overlain by intermediate to mafic volcanics, and all are intruded by common, subconformable, gabbro and porphyritic gabbro bodies. The felsics are thought to represent a volcanic centre. North of it, a highly deformed, gabbroic to tonalitic complex cut by mafic and ultramafic dykes is thought to be pre-Yellowknife Supergroup (EGS 1992-16). All these earlier Archean rock types are invaded along the north and south edges of the Segment by mixed, diorite/gabbro plutonic complexes. These in turn are cut by granitic dykes related to late Archean granitoid plutons which flank the Segment to the north and south and pinch it off to the NE.  To the west, a NNE-trending fault brought a wedge of fine clastic metasediments, of uncertain stratigraphic postition within the Yellowknife Supergroup, into contact with the volcanics. The wedge or belt is less than 1 km across, it's eastern limit defined by late Archean plutonic rocks."
086ISE0001,220,2,"Proterozoic diabase dykes of 2 generations cut all other lithologies. The most abundant are NNW to NW-trending dykes of the Mackenzie swarm.  The Takijuq H-41, or Hood 41, deposit is in an area of predominantly mafic volcanic rocks south of the felsic centre, invaded by both mixed plutonic rocks and late granitic rocks. The deposit is hosted by andesites and to a lesser extent by felsics, and follows the contorted, NNE-trending contact between them. The felsics form a wedge between the host andesitic unit to the NW and a major unit of amygdaloidal andesite to the SE (thought to be stratigraphically below). A granitic intrusive body (late Archean?) cuts off the NE end of the felsic wedge and the sulphide zone, and granitic rocks of a mixed diorite/gabbro plutonic complex are exposed 60m west of the deposit and cut it off to the SW at depth.  Regionally, the deposit is far out on the SE limb of a SW-plunging, macro-syncline whose axial plane strikes NE and dips steeply SE.  Regional metamorphism to lower greenschist grade has been overprinted by contact metamorphism to lower amphibolite grade. The host massive and pillowed andesites are now well-foliated and chloritic. The host felsics are now mica-chlorite-sericite-quartz schists, locally exhibiting chlorite and sericite bands (possible remnant tuffaceous banding), and rarely hosting sericitized fragments. Massive magnetite at the contact between granitic rocks of the complex and the sulphide layer is thought to derive from a contact metamorphic reaction in the sulphide layer.  The sulphides are massive at the NE end and stringer to massive at the SW, in a layer at least 120 m long and 25 m wide, and intersected to 200 m down-dip."
086ISE0001,221,3,"Surface exposure is a 61 x 15 m gossan which yielded chip samples assaying up to 4% Cu and 10% Zn, and grabs up to 6% Cu, 5% Zn and 144 g/t Ag. Drilling in 1975 cut slightly lower grades over 8 to 38 m widths. Subsequent drill results were not reported but in 1991 Minnova announced reserves in two zones, 900,000 tonnes in Zone 41 grading 3.2% Zn, 1.4% Cu and 12 g/t Ag, and 1,100,000 tonnes in Zone 41A grading 3.3% Zn, 2.4% Cu and 16 g/t Ag."
086ISE0002,222,1,"The Takijuq-Hood deposits lie in the northern Slave Province, in the Takijuq Lake-Hood River Supracrustal Belt, a 125 km long, NNE-trending belt of Archean Yellowknife Supergroup mafic to felsic volcanics and various intrusives into them. At its north end, the Belt is only a few kilometres from the southern end of the Anialik River Supracrustal Belt, and its south end apparently adjoins the north end of the Point Lake Belt (EGS 1992-16). Near its south end, at Takijuq Lake, the belt widens into an ENE-trending segment 8 km long and 1.5 km wide. This Takijuq South Segment hosts the Takijuq-Hood deposits and showings.  The Segment contains a greater proportion of felsics than the rest of the belt. The felsics are under and overlain by intermediate to mafic volcanics, and all are intruded by common, subconformable, gabbro and porphyritic gabbro bodies. The felsics are thought to represent a volcanic centre. North of them, a highly deformed, gabbroic to tonalitic complex cut by mafic and ultramafic dykes is thought to be pre-Yellowknife Supergroup (EGS 1992-16). All these earlier Archean rock types are invaded along the north and south margins of the Segment by mixed diorite/gabbro plutonic complexes. These in turn are cut by granitic dykes related to late Archean granitoid plutons which flank the Segment to the north and south and pinch it off to the northeast.  To the west, a NNE-trending fault zone and cross-faults have brought wedges of fine clastic metasediments, of uncertain stratigraphic position within the Yellowknife Supergroup, and blocks of late Archean plutonic rocks into contact with the volcanics.  Proterozoic diabase dykes of two generations cut all other lithologies."
086ISE0002,223,2,"The most abundant are NNW to NW-trending dykes of the Mackenzie swarm.  The Takijuq H-10, or Hood 10, deposit is in the felsic dome. This consists mainly of massive to well-foliated quartz-eye rhyolite, rhyolite agglomerate, rhyolite tuff and dacite. Regionally the felsics are underlain by mafic flows and tuffs with intercalated carbonate beds, and overlain by laterally extensive, pillowed and massive mafic flows and tuffs. The felsics are restricted in areal extent and may represent the explosive end stage of the first of two cycles of volcanism in the Takijuq Belt (Gill 1976).  A narrow, mafic to ultramafic dyke which is calcareous, chlorite-rich and locally serpentinized, cuts the H-10 deposit in the vicinity of DDH H-10-5, trending 040 - 050 degrees (parallel to the main penetrative foliation).  Late Archean granitic rocks are in intrusive contact with the felsic volcanics 150 m south of the deposit, and in NW-trending fault contact with them 150 m west of the deposit. Emplacement of these plutonic rocks was preceded by at least two phases of deformation, the first producing a major syncline, the second only minor folds, and lower greenschist facies regional metamorphism, and was accompanied by contact metamorphism which raised the grade of nearby rocks, including the deposit, to lower amphibolite.  A number of 1 - 2 m wide Proterozoic diabase dykes cut the deposit area.  The main deposit consists of four separate, possibly en echelon, pencil-shaped lenses of massive sulphides, possibly representing four separate mineralizing events. The lenses plunge NNE at 60 degrees, and the deposit as a whole is about 270 m long, on average approximately 12 m but up to 70 m wide, and about 250 m deep, based on information to 1976."
086ISE0002,224,3,"It strikes SE, dips subvertically NE, and probably faces NE, although other lithological contacts in the vicinity strike east. Exposure is poor and structural interpretation was preliminary and inadequate in the latest available reports (1976), which suggest that the deposit lies on the SE limb of a major NE-trending syncline affected by minor north trending folds.  The sulphides are hosted mainly by a laterally extensive unit of amygdaloidal andesite, over and underlain by cherty rhyolite which is a subordinate host. Chloritic alteration is locally heavy, especially to the north. A well-defined alteration pipe is absent (Gill 1976), although stringer sulphides to the west underlie the massive, banded and non-banded zone. The sulphide lenses comprise massive to disseminated to stringer pyrrhotite-chalcopyrite-pyrite-sphalerite-(galena)-(marcasite), with clear mineralogical and metal zoning indicating Cu-rich zones underlying Zn-rich zones. A hundred and fifty metres north of the main H-10 zone is a second sulphide deposit, relatively Pb-Zn rich and known as the 10b zone. It is characterized by pyrite-pyrrhotite-sphalerite-galena as amygdule cores and partial infillings.  Grabs assaying up to 0.51% Cu, 2.1% Pb, 12% Zn and 48 g/t Ag stimulated interest in the showing. Later drill intersections assayed as much as 8% Cu, 2.7% Pb, 19% Zn, 65 g/t Ag and 4 g/t Au over 1 m to 16 m core lengths, and selected 1991 drill intersections are 5.7% Cu and 5.1% Zn over 46 m, and 3.5% Cu and 3.3% Zn over 36 m.  A 1991 estimate of drill-indicated reserves is 1.2 million tonnes grading 4.1% Cu, 4.4% Zn and 27 g/t Ag (Minnova Inc, Toronto, Press Release, Nov 29/91)."
086KSW0006,225,1,"Bornite, chalcopyrite, pyrite, hematite and carbonate found in vugs, fractures and vein breccia in 2 quartz stockworks cutting dacite of the Aphebian Cameron Bay Group.  Work done on the showing includes: 1921: discovery 1950-57: test pitting, sampling, diamond drilling (in 1957, 3,473 feet of widely spaced diamond drilling was done) 1968-69: geological mapping, prospecting, trenching, radiometric, EM and magnetic surveys were done. Diamond drill inferred resources are listed as 100,000 tons at 8.4% copper to 275 feet."
086NNW0070,226,1,"Chalcocite and malachite occur in a brecciated shear zone in basalts of the Neohelikian Copper Creek Formation - Coppermine River Group. The showing area was worked from 1967-68 and included prospecting, geological mapping, geophysical surveys and diamond drilling. Drilling indicated a deposit having the dimensions of 107 m x 1.2 m x 46 m deep with an estimated resource calculated at 125,000 tons at 2% copper to a 600 foot depth."
086NSE0014,227,1,"Chalcocite and bornite occur as narrow veinlets in fault hosted quartz veins that crosscut brecciated basalts of the Coppermine River Group.  From 1967-69 the showing was subjected to prospecting, geological mapping, IP survey and 22 diamond drill holes. A tonnage and grade of 131,000 tons at 2.89% copper (1968) was based on 8 drill holes totalling 840 feet."
086NSE0121,228,1,"Mineralization occurs as a tabular body (1,500 feet long x 35 feet wide) containing chalcocite and some bornite in a fractured and shattered zone along a fault cutting basaltic flowss of the Neohelikian Coppermine River Group.  Work done on the showing includes: 1967-68: EM, IP and magnetic surveys, geological mapping, diamond drilling, airfield and tote road building, milling tests (60% copper concentrate with 4 to 5 oz/t silver and 92% copper recovery). 1971-72: gerochemical work 1981: results of the geochemical work under study  Resources calculated are listed as 4,162,000 tons at 2.96% copper, 10% dilution. The estimated tonnage is to 600 feet, open at depth and along strike to the SW."
086ONW0084,229,1,"Mineralization consists of chalcocite, minor bornite, chalcopyrite and pyrite in a highly fractured/brecciated basalt of the Neohelikian Coppermine River Group. Mineralization is exposed intermittantly over 213x4.5 m. Resources calculated in 1969 are listed as 1,000,000 tons at 2.5% copper."
086OSW0097,230,1,"The Muskox Intrusion is a layered ultramafic body containing chromium, copper, nickle plus minor platinum and palladium.  The showing is situated in the northwestern portion of the Bear Structural Province and is of Mesoproterzoic age.  A 500 metre wide feeder dyke to the intrusion is traceable for about 55 kilometres south-southeasterly from the Coppermine River while a funnel-shaped, layered complex is exposed for 50 kilometres north of the Coppermine River.  The width of the complex varies but has a maximium width of 9 kilometres.  Exploration has been targeted on the central layered portion and the marginal sulphide zones in the complex.  Sulphides along the margin are generally greater than 1 percent and form two thick (60 to 350 metre) gossanous bands.  At the intrusive/country rock contact layers to pods of massive pyrrhotite (minor pentlandite and chalcopyrite) occurs.   A chromite seam (38 centimetres thick) is exposed at the center of the intrusion and a resource figure is reported for this layer (GNWT RWED, MOG Book (1997))."
095ENW0002,231,1,"Lead and zinc sulphides occur as pods, lenses and in fractures in sheared skarn at the contact of Cretaceous quartz monzonite with Cambrian sediments. The main B zone is a vein system with sheared carbonate replaced by sulphides. A resource estimate of 1,635 T/VF at 5.12% lead, 5.42% zinc and 0.71 oz/ton silver was based on mapping, trenching and sampling of the B zone in 1974. Diamond drilling was done in 1975."
095FNE0013,232,1,"Mineralization exists as veins of massive argentiferous galena and sphalerite plus tetrahedrite, minor chalcopyrite in a shear zone hosted by cherty dolostone of the Ordovician Whittaker Formation.  The showing is situated at a facies change between platformal carbonates and basinal calcareous shales of the Selwyn Basin.   Twelve zones of mineralized veins and and a few stratiform deposits giving a total strike lenght of 20 kilometres.    Work done on the showing includes: 1928: discovery 1959-60: staking, mapping and trenching 1966-69: stripping, geophysics, diamond drilling, two adits were driven with crosscuts 1970-74: diamond drilling, drifting, raises driven, soil geochemical sampling, metallurgical testing,  1974-75: recalculation of reserves, surface and underground diamond drilling and tunnelling 1981-82: preproduction development, a 1,000 ton per day mill erected  A resource estimate of 2,143,000 tons (proven, probable and possible) at 10.9% lead, 13.5% zinc, 0.52% copper, 0.087% cadmium and5.58 oz/t silver was listed in 1974. In 1982 a resource calculation for Zone 3 was given as 1,629,000 tons proven and possible at 11.16% lead, 12.17% zinc, 0.44% copper and 5.4 oz/t silver.  In 1995 the in situ metal inventory was reported to be 565 kt zinc, 502 kt lead and 780 t silver."
095LNE0007,233,1,"The Coates Lake showing has Zambian-type stratiform mineralization consisting of pyrite, chalcopyrite, bornite, digenite, chalcocite, covellite, plus malachite and azurite which is disseminated within beds of Hadrynian limestone and dolomite at the transition between red beds and grey Coppercap Formation limestone of the Hadrynian Coates Lake Group.  The area is known as the Redstone Copper Belt .  The cooper-bearing rocks have a maximum thickness of 110 metres and a strike lenght of 30 kilometres.  Work was done on the showing site from 1960 - 1989 (when it was reassessed). Work includes: geochemical sampling, geological mapping, geophysics and diamond drilling (including 24,000 feet in 1976-77 by Shell Canada Resources). Tonnage and grade were calculated for the B-1 copper bearing bed that dips 30 degrees W with a strike length of 20,000 feet and continues downdip 8,000 feet.  Diamond drill indicated reserves  are listed as: 37,000,000 tons at 3.9% copper, 0.33 oz/t silver, over a thickness of 3.3 feet OR 20,500,000 tons at 4.2% Cu, 0.27 oz/t silver (1977)."
095MNW0001,234,1,"Mineralization includes pyrite, chalcopyrite, bornite, digenite, chalcocite and covellite in a lensoid Zambian type copper deposit in do;lomites of the Lower Coppercap Formation at the top of the Hadrynian Coates Lake Group within the Keele River embayment. A resource was estimated at 1,200,000 tonnes at 2.7% copper across 12.5 m (1976) - this estimate is based on diamond rilling (? amount)."
095MNW0038,235,1,"June creek north located 1 mile N, keele west and trudy creek 0.75 mile E."
095OSW0006,236,1,"Mineralization consists of sphalerite and galena disseminated in Middle Devonian bitumen-bearing limestone, it also appears to lie along fault zones as fractures and breccia fillings.  Work done on the showing area includes: 1967-74: trenching, geological mapping, geochemical sampling, IP and diamond drilling 1987: sampling.  Potential resources indicated are: 1,000,000 tons at 8-10% lead zinc."
105INE0002,237,1,"Mineralization consists of disseminated pyrite, pyrrhotite and minor chalcopyrite along thin fractures in bedded limey quartzite and shale close to a granitic intrusion.  Work on the showing included prospecting and diamond drilling (786 feet in 5 holes). An inferred resource was calculated at 25,000 tons at 0.5% copper."
105ISE0003,238,1,"Mineralization consists of scheelite and chalcopyrite in garnet-diopside and massive pyrrhotite skarns in Cambro-Ordivician wavy-banded limestone unit adjacent to a Cretaceous quartz monzonite stock.  Work done on the showing includes: 1960-61: staking, geological mapping, diamond drilling 1967: restaking, soil sampling, mapping, magnetic survey 1973: geological mapping, trenching 1977: geological mapping, soil sampling, EM and magnetic surveys and diamond drilling. Diamond drill indicated resources from 1986 are listed as 750,000 tonnes at 1.17% WO3, and an estimated 0.15% copper."
105ISW0018,239,1,"The Howard Pass (XY) deposit is a Silurian aged stratibound sedimentary hosted zinc-lead showing located in the Cordillera Structural Province along the NWT-Yukon Border .  The showing is hosted in a chert, limestone and mudstone (slate) unit termed the Active Member which obtains a maximum width of 50 meters in the center of the unit, thining towards the outer margins.   The unit is situated in a paleo-basin  which allowed concentrations of sphalerite, galena and pyrite to accumulate.  Pyrite is strongly associated with the occurance of sphalerite and galena.  Other minerals associated with the deposit include nickel, colbalt, arsenopyrite, stibnite and selenium.  The Active Member is sub-divided into an upper and lower sequence.  The upper portion of the unit is dominated by  carbonaceous chert while the lower portion is limestone and cherty limestone along with some carbonaceous mudstones (CIMM, Special Volume 37; referenced as V3719).  Mineralization occurs throughout the Active Member with erratic occurances and a decrease in lead and zinc values along the thinner margins.   The footwall sediments consist mainly of carbonaceous mudstone with a reported thickness of 50 metres  while the hanging wall sediments are phosphatic carbonaceous chert.  Both of these units are black in colour and are eith massive to more commonly laminated.  Some sphalerite, galena and pyrite occur within these units but of much lesser concentration then within the Active Member."
105ISW0018,240,2,"Work preformed on the showing include exploration diamond drilling soon after the discovery in 1968.  An all-weather road was constucted in the early to mid 1970s.  More recently , early 1980s,  underground exploration was conducted in order to bulk sample and test (metallugical) the depost.  The showing has a drill-indicated reserve of 59,000,000 tonnes grading 5.4 percent zinc and 2.1 percent lead."
105OSE0001,241,1,"Work done on the showing include: 1962-68: exploration and sampling, geochemistry, mapping and diamond drilling 1973: An adit was opened, crosscuts driven and underground diamond drilling done as well as metallurgical testing 1974-77: environmental and feasibility studies were done 1979-80: diamond drilling, underground bulk sampling and ecological studies  were done  The Mactung showing consists of two zones, in 1983, resources were calculated: Lower zone: 6.1 million metric tonnes minable underground at 1.16% WO3; Upper zone: 17.2 million metric tonnes minable by open pit at 0.78% WO3."
106ASW0002,242,1,"The Bear-Twit showing has been subjected to geochemical sampling and diamond drilling. Resources are listed as 8-10 million tons at up to 5.4% zinc, 2.6% lead and 0.5 oz/t silver. Diamond drilling in 1976 by Bethlehem Copper Corp indicated the deposit to be sub-economic."
106BNE0014,243,1,"This showing is a carbonate hosted zinc-lead deposit in the Grainstone and Basinal Formations of the Hadrynian Little Dal Group. Mineralization consists of sphalerite, galena,  and minor pyrite in breccias of Mississippi Valley Type tabular to pillarlike bodies near stromatolite reefs. Work done on this showing includes geochemical sampling, IP, geological mapping, geophysics, lithogeochem and diamond drilling (at least 89,400 feet in 169 holes). Resources are estimated to be 50,000,000 tons at 4.7% zinc and 0.3% lead . Typical individual diamond drill indicated bodies where zinc is greater than lead include: 56,300 tons at 14.52% Zn-Pb; 95,000 tons at 9.85% zn-Pb and 1,066,800 tons at 4.51% Zn-Pb."
106FSE0002,244,1,"Crest is an iron deposit hosted in the Rapitan Group of glacial-marine sediments containing a 150 metre thick hydrothermally deposited iron formation of Late Proterozoic age.  The Rapitan Group strikes southeast for 640 kilometres and obtains a width of 40 kilometres and has a basal unconformity related to rifting in the Late Proterozoic.  This group of glacial-marine sediments is conformably overlain by Cambrian aged shales and carbonates.   The Crest showing is located in the northern portion of the Rapitan Group in the Snake River area and is the most iron-rich portion of the Rapitan Group.  The iron formation consists of 10 iron-rich layers (each about 24 metres thick)  characterized by hematite-jasper pistolite, pod and wave rhythmites.  The laminae within the rhythmites are of millimetre to centimetre thick.  Hematite is the iron-ore mineral within the showing which has a resource of 5.6 billion tonnes grading about 47.2% iron.      The region contains the third largest deposit of iron in North America with a total resource estimate of greater than 18.6 billion tonnes.  Iron concentration was first note around the turn of the century (1906) during the Klondike gold rush by prospectors.  But it was not until 1961 that an iron-enriched strata was discovered in the Rapitan Group of sediments.    During the 1960's at least 3048 metres (25 diamond drill holes) of diamond drilling, channel sampling and bulk sampling  were completed in the Snake River basin."