Lac La Ronge, NTS Area 73P/731 Frrst Edition, 1985

Saskatchewan Report 225 Energy and Mines

Saskatchewan Compilation Bedrock Geology Map Series: Geological Survey Lac La Ronge, NTS Area 73P/731 Frrst Edition, 1985

Printed under the authority of the Minister of Energy and Mines Although the Department of Energy and Mines has exercised all reasonable care in the compilation, interpretation and production of this report, it is not possible to ensure total accuracy, and all persons who rely on the information contained herein do so at their own risk. The Department of Energy and Mines and the Government of Saskatchewan do not accept liability for any errors, omissions or inaccuracies that may be included in, or derived from, this report. Geological Notes The Lac La Ronge map area is underlain by early Wollaston Domain Proterozoic crystalline basement rocks of parts of four High-grade granite gneisses (sensu stricto) and granitoid lithotectonic domains of the 'Trans-Hudson Orogen', and gneisses (Wfn), minor metagabbro-metadiorite (Wbd) and a number of subdomains divided on the basis of amphibolite (Wm) of this domain are the only difference in structural and/or lithological character (see documented Archean basement in the map area. These inset map). These rocks have moderate to good exposure units are unconformably overlain and tightly infolded with beneath a thin and sporadic Pleistocene glacial drift Aphebian supracrustal rocks of the 'Sandfly Lake Group' cover, except in a zone up to 18 km wide north of the (Money, 1968) and Wollaston Group. The Sandfly Lake Phanerozoic/Precambrian boundary where the drift is as Group comprises biotite schists and gneisses (Wvn) of much as 20 m thick (borehole D.M.R. Morin Lake 4-76, probable volcano-sedimentary origin and immature meta Lsd 10-4-71-25W2, in Fuzesy, 1980). The south is arkosic psammites and metaconglomerates (Wm), which underlain by unmetamorphosed Phanerozoic sedimentary in the Needle Falls area locally comprise a thin basal rocks covered by a blanket of drift as much as 85 m thick continental to fluviatile sequence. These are in places (borehole D.M.R. Morin Lake 11-77, Lsd 13-1- unconformably overlain by mature, passive margin 70-26W2, in Fuzesy, 1980). The Phanerozoic map is based quartz-pebble metaconglomerates (Wry) and largely on work by Fuzesy (1980), with additional orthoquartzites, feldspathic quartzites and aluminous information from borehole and diamond-drill hole data muscovite pelitic schists (Wq) of the Wollaston Group (Canadian Occidental Petroleum Ltd., 1978; Great Plains 'Meyers Lake-type' rocks (Money, 1968), Higher grade Development Co. of Canada Ltd., 1968, 1970). pelitic gneisses (Wpsn) occurring in this vicinity are probably also Aphebian but some may be Archean. Contacts between Archean basement and Aphebian Phanerozoic Rocks cover are highly strained, with local tectonic elimination of To the west of Lac La Ronge, the Phanerozoic rocks parts of the cover succession. The granitic basement also consist of a lower elastic unit, a middle carbonate unit and contains local high strain zones parallel to the Needle an upper elastic unit, each separated by an erosional Falls Shear Zone. unconformity. The Meadow Lake Escarpment, just south of the map area, marks the southeast boundary of the Rottenstone Domain carbonate unit. To the east of this only the two elastic The Wathaman Batholith comprises coarsely megacrystic units are present. pink quartz monzonite-monzogranite and poorly to non megacrystic pink-grey granite and granodiorite (Rgp). The lower elastic unit of the Cambrian Deadwood These are irregularly distributed, have complex locally Formation rests nonconformably on relatively soft gradational contacts, and cannot be consistently weathered Precambrian rocks. The unit consists of grey subdivided on the basis of available data. Much of the to brownish-grey glauconitic quartzose sandstones with batholith is highly xenolithic and migmatitic. Zones minor shales and conglomerates (Fuzesy, 1980). incorporating large screens (possible roof pendants) and Deposition occurred during the eastward transgression of trains of hornblende gneiss-amphibolite and tonalite Paleozoic seas onto the Precambrian surface (Fuzesy, migmatite country rock are generally characterized by 1980). inequigranular pegmatitic and aplitic phases of the batholith. Older, metasomatized and injected country The middle carbonate unit, deposited in Middle Devonian rocks form an extensive and complex metasomatic supratidal and subtidal environments (Fuzesy, 1980), aureole adjacent to the highly irregular eastern margin of unconformably overlies either the Deadwood elastics or the batholith and its satellitic bodies. Most of the batholith the Precambrian basement where the elastics are absent. is weakly to moderately foliated, but a westward gradation The unit comprises lower and upper members of the into strongly flasered and comminuted augen gneisses Meadow Lake Formation. The Lower Member includes (Rgpx), and thence into laminated mylonitic gneisses, primarily grey to brown argillaceous and silty dolomites occurs over an interval of several hundred metres (Fuzesy, 1980). Simpson (1975) has suggested that a adjacent to the Needle Falls Shear Zone. Regular glacially disrupted outcrop on the south shore of Morin compositional banding in the laminated mylonites partly Lake is part of the Winnipegosis Formation, although it derives from tectonic attenuation and transposition of may belong to the Lower Member. The Upper Member, main phase megacrystic quartz monzonite, aplitic and present only in the extreme southwest, comprises three pegmatitic sheets, and mafic xenoliths. Strongly flasered distinct units of limestone, dolomite and mudstone and refolded pink megacrystic-augened monzogranitic (Fuzesy, 1980). gneisses (Rnax) around Black Bear Island Lake may represent pre-Wathaman Hudsonian intrusives or The upper elastic unit consists of lacustrine-fluvial, Archean basement. However, similar highly strained rocks fluviomarine, and marine sandstones and shales of the in the Besnard-Morning Lakes area (Rna) locally appear Lower Cretaceous Mannville Group (Simpson, 1975). transitional to less deformed porphyritic granite Several outcrops of sandstone containing small amounts granodiorite of the Wathaman Batholith and may of coal are exposed on the south shore of Wapawekka represent localised high-strain zones. Age relations in Lake (Langford, 1973). both areas are unresolved. The Tonalite-Migmatite Complex comprises variably a high-level tectonic slice structurally overlying the migmatized supracrustal gneisses (Rng) and subordinate, possible forearc assemblage of the Maclean Lake Belt to compositionally heterogeneous, plutonic bodies (Rgl and the southeast. Rgt). The supracrustal paleosome is mostly psammitic to psammopelitic biotitic metagreywacke with subordinate The Crew Lake Belt and Nemeiben Zone comprise pelites, hornblendic gneisses, amphibolites (Rm), calc predominantly biotitic pelitic to psammitic silicates and meta-arkoses, interpreted as arc-derived metagreywackes and other volcanogenic metasediments volcanogenic elastics and volcaniclastics. These are (Lsn). Acid volcanics and volcaniclastics are important transitional to similar but generally less migmatized rocks locally, as are amphibolites, calc-silicate rocks and of the La Ronge Domain, but contrast markedly with the hornblende gneiss of probable volcanic origin (Lm), and Wollaston Group. Neosomal components include two polymictic metaconglomerates (Lon). A volcanic to suites: 1) a pre- to synkinematic suite of strongly foliated sedimentary transition occurs northwestwards across the and folded quartz dioritic-tonalitic-trondjemitic Crew Lake Belt. The Nemeiben Zone, which is part of the granodioritic gneisses together with less deformed later 'La Ronge Horseshoe' (Pearson, 1973), mainly comprises rocks of a similar compositional range (Rgt), and 2) a late strongly foliated pre- to early synkinematic granodioritic synkinematic suite of pink leucogranites, pegmatites, and granitic gneisses (Lgn) interleaved with supracrustal rocks megacrystic and non-megacrystic monzogranites (Rgl) and complexly deformed by at least two postfoliation fold which are considered mostly coeval with the Wathaman episodes. This early plutonic complex is characterized by Batholith but which may include components of at least predominantly biotitic rock types but includes extensive two different ages. Both suites form elongate and folded hornblende-bearing granodiorite-quartz diorite-tonalite, as intrusive bodies on all scales, as well as pervasive well as undifferentiated large and small zones of quartz neosomes in the migmatitic gneisses. monzonite-granite (Lqm). Discrete, possibly later, plutons in the Nemeiben Zone include little-deformed to massive The Birch Rapids Straight Belt, which forms the eastern mafic-ultramafic bodies (Lbd and Lum) and quartz diorite part of the Tonalite-Migmatite Complex, is marked by granodiorite (Lqd). Bodies of pink, commonly regular strongly linear structural and aeromagnetic trends, megacrystic, granite-quartz monzonite (Lqm) in this zone and can be traced to the south under the Phanerozoic are similar in character and possibly age to the Wathaman cover as a distinct aeromagnetic feature. This belt is Batholith and related bodies in the Rottenstone Domain. lithologically similar to the remainder of the complex but The has a high-strain planar kinematic fabric and transposed plutons of the Central Metavolcanic and Crew Lake are generally composite, compositionally subparallel layering. Between Clam Lake and eastern Belts Black Bear Island Lake it mainly comprises only mildly heterogeneous ovoid bodies. Many have an outer mafic quartz diorite-granodiorite zone which grades into or is migmatized metagreywackes; minor hornblende gneisses; intruded by a quartz monzonite-granite core. Most of the early, strongly foliated to mylonitic, granitic sheets; and a plutons are massive or only moderately foliated, except suite of later less foliated but highly boudinaged leucogranites and pegmatites. Protomylonite-mylonite locally, and may be equivalent in age to late ovoid bodies zones occur locally. The straight belt is thought to have in the Nemeiben Zone. Others, though little deformed, developed by both pure shear flattening and simple shear may be coeval with intensely foliated phases in the displacement. South of Trout Lake, the straight belt structurally lower and more deformed infrastructure of the includes major bodies of flasered to mylonitic granite Nemeiben Zone. (e.g., Trout Lake Pluton}, including Wathaman-type augened megacrystic monzogranite, which to the east The Nut Bay Belt is lithologically similar and appears passes transitionally into less deformed to massive transitional to the Nemeiben Zone but has more strongly equivalents (Lqm and undifferentiated parts of Lgn). From foliated biotitic and/or hornblendic granodioritic gneisses (Lgn). These are intercalated with subordinate Mackintosh Lake northeastwards, the straight belt is supracrustals consisting predominantly of hornblende intruded and supplanted by little-deformed and generally uniform pink biotite granodiorite-granite, as well as gneiss and amphibolite of metavolcanic or metavolcaniclastic derivation, with subordinate biotitic related pegmatite of the Hickson Lake Pluton. metasediments. Mafic-ultramafic plutons occur locally. La Ronge Domain Some of the fine-grained, strongly foliated and laminated amphibolites (Lmx), as in the Lynx, Sulphide and Hunt The Central Metavolcanic Belt features predominantly Lake areas, are strained derivatives of the mafic-ultramafic calc-alkaline to tholeiitic mafic to felsic metavolcanic plutons. Mafic schists occurring elsewhere may be rocks, proximal volcaniclastics and epiclastics, and similarly derived. interlayered volcanogenic metasediments intruded by granitic to ultramafic plutons. These rocks are of Early The Maclean Lake Belt is mainly a mixed suite of Proterozoic age (c. 1880 Ma; Van Schmus et al., 1985) psammitic to psammopelitic metagreywacke (LMsn), and the belt is considered to be a subduction-generated polymictic metaconglomerate (LMon) and hornblendic to island arc remnant. The metamorphic grade is low and amphibolitic gneisses (LMm), which may represent a the belt appears relatively less deformed than other parts telescoped forearc basin assemblage. They are of the domain. The belt is possibly allochthonous, forming structurally, and probably stratigraphically, overlain by

2 locally conglomeratic molasse-type meta-arkoses, deform flat-lying foliation and coeval isoclinal folds of two granitoid meta-arkoses and derived granitic-pegmatitic generations (01 and 0 2), which are correlated with early neosome of the Mclennan Group (LMr, LMrg), which are fold-foliation forming episodes in the La Ronge Domain. probably partly equivalent to the Sickle Group in In much of the Glennie Lake Domain, the late folds are Manitoba. The Haugen-MacKay-Hedben Lakes area relatively open and the early foliation is gently dipping. In includes abundant polymictic metaconglomerate which the southwest, a change in gross structural style from the mostly contains volcanic as well as granitic clasts in a La Ronge Domain roughly coincides with the Stanley mafic greywacke-type matrix. The metaconglomerates are Shear Zone discontinuity. Northeast of Guncoat Bay, dominantly arkosic adjacent to the infolded outlier of the there is a lithological and structural transition between the Mclennan Group northeast of Hebden Lake and steeply dipping Nut Bay and Maclean Lake Belts and the elsewhere. In the MacKay Lake area, quartz-eye granite Wapassini Allochthon of the Glennie Lake Domain, where porphyry sheets (LMg) intrude the metaconglomerates the northeast continuation of the late brittle Stanley Fault and also appear to provide detritus to some of the arkosic system forms an arbitrary domain boundary. conglomerate units. The Wapassini Allochthon structurally overlies and Apart from the albite-bearing Bridgeman Lake Pluton includes refolded parts of the Guncoat Gneisses (Gxg) (LMga), felsic igneous rocks are a minor component of east of the Stanley Shear Zone. It is considered to be a the Maclean Lake Belt, in contrast to the remainder of major allochthonous tectonic package (nappe), rooted in the La Ronge Domain. The supracrustal rocks are more the Nut Bay and Maclean Lake Belts, which incorporates highly migmatized in the northeast and much of the belt highly appressed, complexly refolded isoclines and contains a high proportion of anatectic mobilizate. The formerly flat-lying foliation. The allochthon comprises Maclean Lake metagreywacke assemblage is probably at mixed psammitic to pelitic metagreywackes, minor least in part coeval with lithologically similar rocks metaconglomerates, layered to homogeneous elsewhere in the La Ronge Domain. metavolcanics, volcaniclastics and calc-silicates equivalent to those in the Nut Bay and Maclean Lake The Maclean Lake Belt is intensely deformed: at least Belts. Minor ultramafic and metagabbroic bodies occur two fold-foliation forming events, accompanied by locally. Associated quartz dioritic to granitic orthogneisses localized high-strain zones along fold limbs, produced the (Ggn) resemble those of the Nut Bay Belt (Lgn) but are dominant northeasterly structural grain. A pervasive commonly less homogeneous and more migmatitic; an downdip-stretching lineation is characteristic. The belt is unknown proportion may be reconstituted from considered to comprise a series of fold-thrust packages supracrustal rather than plutonic protoliths. associated with extreme crustal shortening. The Mclennan Group is considered to occupy the core of a The Guncoat Gneisses, which form the sole of the complex, overturned, isoclinal synform tectonically Wapassini Allochthon, are mylonitic rocks and tectonic overridden by the older Central Metavolcanic Belt along schists considered to be derived from earlier the Mclennan Tectonic Zone. psammopelitic diatexites, and to a lesser extent from plutonic protoliths subsequently recrystallized at high The Meraste Zone differs from the Nut Bay Belt and grade. They are considered to be the main component of Nemeiben Zone in comprising generally more mafic and an early-tectonic high strain zone which forms the sole or commonly richly hornblendic quartz diorite and lower detachment zone of the Wapassini Allochthon. granodiorite gneisses with abundant amphibolite and amphibolite migmatite, more akin to rocks within the The lskwatikan Subdomain, which structurally underlies Stanley Zone and adjacent parts of the Glennie Lake the Guncoat Gneisses sole, mainly comprises variable, Domain. This is reflected in a distinctive aeromagnetic well-foliated and commonly migmatitic hornblende and/or signature. The zone is gradational into the Stanley Shear biotite quartz diorite, tonalite, granodiorite and granite Zone with increasing intensity of planar fabrics and orthogneisses (Ggl and Gdl). Hornblende gneiss and increasing incidence of protomylonitic-mylonitic gneisses. fine- to coarse-grained amphibolite paleosome remnants range from isolated schlieren to major semicontinuous Strongly sheared fine-grained to mylonitic rocks (Lxt) migmatitic and nonmigmatitic zones (Gm) . Also occurring occur near the boundary of the Meraste and Nut Bay are later minor to abundant injections or bodies of biotite Zones, but no well-defined tectonic discontinuity is bearing megacrystic quartz monzonite, granite (Gqm), evident, except in the north. Many of these highly strained and equigranular leucogranite and pegmatite of several rocks are derived from plutonic protoliths, while others possible ages. These range from relatively uniform may be supracrustal. massive to intensely foliated. The indicated lithological distinction between units Ggl, Gdl and grossly similar orthogneisses of the La Ronge Domain (Lgn) and Glennie Lake Domain Wapassini Allochton (Ggn) is of doubtful validity, except The Glennie Lake Domain is characterized by complex that the latter are at a higher structural level. Unit Gdl arcuate to closed structural trends considered to be due includes rocks generally described as relatively to Type 1 and 2 fold interference of northerly (03) and homogeneous hornblende-bearing quartz diorite and northeasterly (04) large amplitude major folds. These granodiorite-tonalite plutonics, as well as local quartz

3 monzonite-granite and complex migmatitic zones. Unit The Kahn 18 vein, less than 200 m south of the 21 zone in Ggl is generally lithologically more varied, the original discovery area, is being evaluated as a inhomogeneous and dominantly biotitic, and may include possible supplement to the 21 zone production. components older than unit Ggl. In places, as for example Mineralization is contained in a sheared ('ribbon') quartz immediately north and south of Wapawekka Lake, the vein that infills a northeast-trending shear fracture cutting unit includes abundant later homogenous plutonic biotite/ monzonites of the Star Lake Pluton. The wall rocks are hornblende granodiorite (Ggd), quartz monzonite and epidotized and hematized and the greatest concentration granite (Gqm). of gold tends to be towards the footwall side of the vein. The zone has been traced along strike for 250 m and Highly strained, protomylonitic and blastomylonitic rocks drilling has intersected 41.8 g/t Au over 0.5 m (Thomas, of the Nistowiak and Hunter Bay gneisses (Gxn and Gxh) 1984). are largely derived from varied metaplutonic and migmatitic protoliths. These include mafic to mesocratic The Rush Lake {Pie claims) zone is also undergoing quartz diorite-tonalite-granodiorite, mesocratic to evaluation as a 21 zone production supplement. The main leucocratic pink megacrystic and non-megacrystic area of mineralization is in a 1 to 3 m wide, massive, white granite-quartz monzonite, leucogranite and pegmatite and to grey quartz vein that is roughly conformable to a local heterogeneous migmatites comprising psammitic to northeast-trending shear zone which dips steeply to the pelitic paleosome and plagioclase-porphyroblastic tonalite southeast. The shear zone can be traced up to 3 km along neosome. These gneisses are strongly foliated, 'beaded', strike, predominantly through diorites of the Star Lake augened and banded/laminated, and are similar in Pluton. Mineralization includes pyrite, chalcopyrite and character to the Guncoat Gneisses, but dissimilar insofar visible gold which is associated with chlorite-rich seams. as most are considered to have plutonic protoliths. In 1970 a small operation crushed 20 tons of ore from the Conversely some areas designated biotitic gneisses (Gsn) main pit area. Drilling has indicated an ore zone with a in the lskwatikan Subdomain may also be tectonically strike length of 60.9 m, width of 1.2 m and depth of 30.5 m derived rocks similar to the Guncoat, Nistowiak and and containing reserves of 5 763 t grading 13.03 g/t Au Hunter Bay gneisses. {Thomas, 1984).

Basic to intermediate metavolcanics (Gvb), intermediate The Tamar showing occurs in a 4.5 to 24 m wide to acid pyroclastics and epiclastics (Gve), and commonly northeast-trending shear zone that has been traced for conglomeratic meta-arkoses of the Wapawekka Lake area 430 m along the contact between metavolcanics to the are generally at lower metamorphic grade and apparently west and diorites of the Star Lake Pluton to the east. less highly deformed than in the remainder of the Glennie Mineralization exists in pyritized quartz veins and lenses Lake Domain. within the commonly chloritized and carbonatized rocks of the shear zone. Composite chip samples assayed 2.7 g/ t Au and 0.7 g/t Ag over 0.9 m (Thomas, 1984). Economic Geology In the Sulphide Lake area, mineralization is predominantly In recent years, mineral exploration in the Lac La Ronge characterized by stratiform-type gold occurrences map area has been concentrated on gold, primarily in the comprising early concordant quartz-sulphide veins within Central Metavolcanic Belt (particularly around Star Lake shear zones. The shear zones cut felsic volcanic and also in the Sulphide Lake area). Both vein- and volcaniclastic sedimentary sequences and related stratiform-type gold occurrences are present, with vein subvolcanic porphyritic intrusives and sill-like gabbroic type deposits more common in the Star Lake area and intrusives. The concordant mineralization is associated stratiform-type deposits predominant in the Sulphide Lake with carbonaceous 'lean' sulphide-facies iron formation area. Vein-type deposits in the Star Lake area have argillites. The more limited discordant mineralization recently comprised the more advanced exploration and comprises tension fracture-fillings and axial plane development stages of gold prospects. Most of the gold fracture-fillings. The Studer A and C zones are the most showings occur in or adjacent to the Star Lake Pluton. significant gold occurrences in the Sulphide Lake area. The joint Starrex/SMDC 21 zone is planned to go into Concordant mineralization at the A zone includes gold, production in mid-1987 with a 200 t/day mill. The 21 zone arsenopyrite, pyrite, pyrrhotite and minor chalcopyrite in mineralization, which has preliminary drill-indicated quartz veins and lenses associated with easterly trending reserves of 209 300 tat 17.14 git Au {Thomas, 1984), shears. Drilling of the A zone indicated a 2.4 m wide and occurs in a dilative zone within steeply dipping northeast 230 m long zone reaching a depth of 230 m with trending shear zones cutting monzonites of the Star Lake estimated reserves of 160,000 tons grading 0.22 oz./ton Au Pluton. Numerous mafic to felsic dykes are broadly (SMDI 73-P-7-SW Au-10) 1. The Studer C zone comprises conformable to the shear zone and, along with the irregular quartz veins and stockworks within highly plutonic rocks in the area, range from moderately foliated, deformed felsic volcaniclastics with essentially no iron cataclastic and protomylonitic to mylonitic. The formation present. Mineralization includes gold, mineralized zone of relatively massive, undeformed quartz and euhedral pyrite has a strike length of 80 m and depth 1saskatchewan Mineral Deposits Index, Saskatchewan Energy of 130 m, with a moderate to steep southwest plunge. and Mines, Regina.

4 arsenopyrite, pyrite and rare galena in quartz veins that the Anglo-Rouyn deposit is located. The disseminated occur both parallel to the earlier foliation and along later sulphides have a possible syngenetic origin, while the axial plane fractures of northerly plunging folds. Drilling veins probably originated from hydrothermal solutions indicated reserves of 18,000 tons averaging 0.4 oz./ton Au concentrated along fracture zones by fracture-filling and (SMDI 23-P-7-SW Au-10) from three parallel zones in an partial replacement. area measuring 60 by 45 m. The Nemeiben Lake Ni-Cu deposit comprises an east Northeast of Sulphide Lake, the Preview Lake North and zone with a 1973 estimate of 2,273,975 probable tons South zones are associated with sheared gabbroic sills grading 0.61 percent Ni and 0.38 percent Cu with an that intrude felsic volcanic-volcaniclastic rocks. The North additional 1,325,280 possible tons and open pit ore of zone comprises pyrite, arsenopyrite and rare chalcopyrite 5,476,000 tons at 0.34 percent Ni and 0.18 percent Cu as disseminations and veinlets in quartz veins and adjacent well as a west zone with open pit estimates of wall rocks along a sheared contact between a gabbroic 1,000,000 tons grading 1.55 percent Cu (SMDI 73-P-6-SE sill and felsic volcaniclastics. Trenching and drilling Ni-2) . The disjointed vein and disseminated sulphide outlined two en echelon mineralized zones with a mineralization, which occurs in sheared areas of an combined potential of 250 tons per vertical foot at a grade ultramafic complex, comprises an earlier nickeliferous of 0.35 oz./ton Au (SMDI 73-P-7-NW AU-1). pyrrhotite, pyrite, chalcopyrite and rare pentlandite Approximately 700 m to the southwest, the South zone is mineralization and a later mineralization consisting of characterized by arsenopyrite, pyrite and rare chalcopyrite native copper, specular hematite and secondary copper mineralization in northeast-trending concordant quartz minerals. The sulphide-rich veins resulted from fracture veins within a sheared gabbroic sill. Trenching indicated a fill and replacement deposition. The disseminated potential of 130 tons per vertical foot at a grade of 0.5 oz.I sulphides probably originated from late magmatic ton Au (SMDI 73-P-7-NW Au-1). crystallization with local remobilization of sulphides along shear zones. As the gold play is currently very active, more up-to-date and comprehensive accounts of the mineralization will be At the north end of Howard Lake, disseminated pyrite, found elsewhere. pyrrhotite, chalcopyrite and pentlandite mineralization has estimated reserves of 60,000 tons grading 1.03 percent Ni, In addition to gold mineralization, the Lac La Ronge map 0.44 percent Cu and 0.044 percent Co (SMDI 73-P-5-SE area contains several disseminated sulphide occurrences Ni-1 ). The mineralization exists in a narrow hornblende with significant Cu and Ni values, plus one past quartz diorite-gabbro-ultramafic complex within a biotite producing mine. The Anglo-Rouyn mine and the quartz diorite-biotite gneiss migmatite. Elizabeth Lake, Nemeiben Lake, Howard Lake and Gochager Lake occurrences all occur in the La Ronge The Gochager Lake Ni-Cu prospect consists of extensive Domain. The Anglo-Rouyn copper mine commenced rusty zones containing pyrrhotite, pyrite, chalcopyrite and mining operations in 1966 with estimated reserves of bornite mineralization with estimated reserves of 2 million tons averaging 2.4 percent Cu and ceased 4,262,400 tons grading 0.295 percent Ni and 0.081 percent operations in 1972 with a final production of Cu mineable by open pit methods, plus an additional 62,227,107 lbs. of Cu, 67,622 oz. of Au and 309,600 oz. of 876,200 tons grading 0.389 percent Ni and 0.093 percent Ag (SMDI 73-P-6-SE Cu-1 ). The sulphide ore occurs as Cu mineable by underground methods (SMDI 73-P-15- lenticular zones up to 30 feet wide, located primarily in SW Ni-1). The mineralization occurs as massive pods, biotitic metasedimentary rocks in close contact with disseminated blebs and fracture-filled veins within the granitic intrusives. The en echelon, doubly plunging ore gabbroic and hornblendite rocks of a small mafic plug zones consist of stringers and ramifying veins of quartz intruding the surrounding metasediments. up to 3 m wide with associated pyrite, pyrrhotite and chalcopyrite veins up to 0.7 m wide. The mineralization The Pitching Lake Cu prospect, located in the Glennie was deposited by fracture-filling and limited partial Lake Domain, is to date the only significant mineralized replacement along a northeast-trending fault zone. The occurrence outside the La Ronge Domain. It comprises ore probably originated from 'metamorphic-hydrothermal' three mineralized zones, consisting of disseminated pyrite, solutions derived from the granitic magma or adjacent pyrrhotite and minor chalcopyrite, that occur along shear metasediments. zones within hornblende gneisses containing lenses and layers of calc-silicate gneiss. The A zone, with indicated The Elizabeth Lake deposit contains disseminated and reserves of 100,000 tons grading 2.6 percent Cu (SMDI veined chalcopyrite, pyrite, pyrrhotite and magnetite with 73-P-8-NE Cu-1), has a surface gossan that forms the top drill-indicated reserves of 6,700,000 tons grading of an irregularly shaped Cu-bearing ore shoot. A shaft 1.5 percent Cu (SMDI 73-P-6-SW Cu-2). The lenticular was sunk to a depth of 42 feet at the southwest end of the zones of mineralization, which are similar to those found A zone. The Band C zones are located 1 and 2 miles at the Anglo-Rouyn mine, occur along fracture zones in a northeast of the A zone respectively. Both of these zones north-northeast- trending metasedimentary gneiss belt contain low-grade copper mineralization; an exploration that is locally intruded by gabbro, quartz diorite and adit to test the mineralization beneath the B zone reached granite. This is the same belt of metasediments in which 235 feet with no significant results. Mineralization was

5 probably derived from syngenetic sulphides that were remobilized during a period of metamorphism and concentrated along sheared and brecciated fault zones.

References2 ____ (1971a) : The geology of the Nemeiben Lake area (east half) and the geology of the mineral Abraham, A. and 1,..ewry, J.F. (1981): La Ronge Project: I. deposits in the Nemeiben Lake - Stanley areas (73-P-6- Geology of the Otter Lake area; Summary of in E and 73-P-7-W), Saskatchewan; Sask. Dep. Miner. Investigations 1981, Saskatchewan Geological Survey; Resour., Rep. 115 (Pt. 2), 178p. Sask. Miner. Resour., Misc. Rep. 81-4, p26-27. ____ (1971b): The geology of the Clam Lake Beck, L.S. (1959) : Mineral occurrences in the area (west half), Saskatchewan; Sask. Dep. Miner. Precambrian of northern Saskatchewan (excluding Resour., Rep. 136, 15p. radioactive minerals); Sask. Dep. Miner. Resour., Rep. 36, 134p. ____ (1972a): The geology of the Clam Lake Bell, K. and Macdonald, R. (1982): Geochronological area (east half), Saskatchewan; Sask. Dep. Miner. calibration of the Precambrian Shield in Saskatchewan; Resour., Rep. 138, 21 p. in Summary of Investigations 1982, Saskatchewan Geological Survey; Sask. Energy Mines, Misc. Rep. 82- ____ (1972b): Anglo-Rouyn Copper Mine, Ore 4, p17-22. Bay, Lac La Ronge, Saskatchewan; Geol. Soc. Am. Bull., v83, p3405-3414. Budding, A.J. (1955) : The geology of the Settee Lake area (east half), Saskatchewan; Sask. Dept. Miner. ____ (1976): The geology of the Nemeiben Lake Resour., Rep. 17, 19p. area (west half) and the La Ronge area (west half), Saskatchewan; Sask. Dep. Miner. Resour., Rep. 152, Canadian Occidental Petroluem Ltd. (1978): unpubl. 18p. drilling report in Assessment File 73114-0005, Sask. Energy Mines, Regina. ____ (1981): Geology of the Lac La Ronge - Hunter Bay - Cartier Lake area, Saskatchewan; Sask. Coombe, W. (1975): La Ronge-Wollaston base metals Miner. Resour., Open File Rep. 81-1, 19p. project; in Summary of Investigations 1975, by the Saskatchewan Geological Survey; Sask. Dep. Miner. Fuzesy, L.M. (1980) : Geology of the Deadwood Resour., p101-109. (Cambrian), Meadow Lake and Winnipegosis (Devonian) Formations in west-central Saskatchewan; ____ (1978) : Wollaston base metals project, Sask. Miner. Resour., Rep. 210, 64p. Duddridge Lake to Meyers Lake area; in Summary of Investigations 1978, Saskatchewan Geological Survey; Great Plains Development Co. of Canada Ltd. Sask. Miner. Resour., Misc. Rep. 78-10, p98-108. (1968) : unpubl. drilling report in Assessment File 73P04-0002, Sask. Energy Mines, Regina. Coombe, W. (1984): Gold in Saskatchewan; Sask. Energy Mines, Open File Rep. 84-1, 134p. ____ (1970): unpubl. drilling report in Assessment File 73115-0005, Sask. Energy Mines, Douglas, R.J.W. (1980): Proposals for time classification Regina. and correlation of Precambrian rocks and events in Canada and adjacent parts of the Canadian Shield, Part 2: A provisional standard for correlating Precambrian Langford, F.F. (1973): The geology of the Wapawekka rocks; Geol. Surv. Can., Pap. 80-24, 19p. area, Saskatchewan; Sask. Dep. Miner. Resour., Rep. 147, 36p. Forsythe, L.H. (1968) : Geology of the Stanley area (west half) (MacKay Lake area), Saskatchewan; Sask. Dep. Lewry, J.F. (1981) : La Ronge Project: II. Geology of the Miner. Resour., Rep. 115 (Pt. 1), 58p. Stanley Shear Zone; in Summary of Investigations 1981 , Saskatchewan Geological Survey; Sask. Miner. Resour., Misc. Rep. 81-4, p28-33.

____ (1983) : Character and structural relations of the 'Mclennan Group' meta-arkoses, Mclennan 2A more complete bibliography for Lac La Ronge, NTS Area 730/ Jaysmith Lakes area; in Summary of Investigations 731 is available from the Saskatchewan Geological Survey, 1983, Saskatchewan Geological Survey; Sask. Energy Regina. Mines, Misc. Rep. 83-4, p49-55.

6 ____ (1984): Bedrock compilation, Lac La Padgham, W.A. (1960): The geology of the Otter Lake Ronge and Wapawekka areas (NTS 73P/731); in area (west half), Saskatchewan; Sask. Dep. Miner. Summary of Investigations 1984, Saskatchewan Resour., Rep. 41 , 34p. Geological Survey; Sask. Energy Mines, Misc. Rep. 84- 4, p34-41 . ----(1963): The geology of the Otter Lake area (east half), Saskatchewan; Sask. Dep. Miner. Resour., Lewry J.F. and Sibbald, T.1.1. (1977): Variation in Rep. 56, 51 p. lithology and tectonometamorphic relationships in the Precambrian basement of northern Saskatchewan; Can. ____ (1966a) : The geology of the Guncoat Bay J. Earth Sci., v14, p1453-1467. area, Saskatchewan; Sask. Dep. Miner. Resour., Rep. 78, 143p. Lowdon, J.A. (1961): Age determinations by the Geological Survey of Canada; Geol. Surv. Can., ____ (1966b): The geology of the Wapawekka Pap. 61-17, 127p. Narrows area (north half), Saskatchewan; Sask. Dep. Miner. Resour., Rep. 87, 113p. Macdonald, R. (1984): Review geology, Forbes Lake vicinity; in Summary of Investigations 1984, ____ (1967): The geology of the Wapawekka Saskatchewan Geological Survey; Sask. Energy Mines, Lake area (north half), Saskatchewan; Sask. Dep. Misc. Rep. 84-4, p50-52. Miner. Resour., Rep. 103, 57p.

Macdonald, R. and Broughton, P. (1980): Geological Pearson, W.J. (1973): Mineral evaluation program; in map of Saskatchewan, provisional edition; Sask. Miner. Summary Report of Geological Investigations Resour., scale 1: 1 000 000. Conducted in the Precambrian Area of Saskatchewan, 1973; Sask. Dep. Miner. Resour., p60-67. Mawdsley, J.B. and Grout, F.F. (1951): The geology of the Stanley area, Saskatchewan; Sask. Dep. Miner. Pearson, W.J. and Froese, E. (1959): The geology of the Resour. Rep. 4, 31 p. Forbes Lake area, Saskatchewan; Sask. Dep. Miner. Resour., Rep. 34, 28p. Money, P.L. (1965): The geology of the area around Needle Falls, Churchill River, comprising the Eulas Ray, G.E. (1981): Geology of part of the Foster Lake Lake area (west half), Sandfly Lake area (east half) and (south) - La Ronge (northwest) area, Saskatchewan; Black Bear Island Lake area (west half), Saskatchewan; Sask. Miner. Resour., Rep. 185, 31p. Sask. Dep. Miner. Resour. Rep. 88, ?Op. Rees, C.J. (1982) : Metamorphism in the Canadian ____ (1967): The Precambrian geology of the Shield of northern Saskatchewan; Sask. Miner. Resour., Needle Falls area, Saskatchewan; unpubl. Ph.D. thesis, Open File Rep. 82-2, 136p. Univ. Alberta, Edmonton, 251 p. Sangster, D.F. (1978): Isotopic studies of ore-leads of ____ (1968): The Wollaston Lake fold-belt the circum-Kisseynew volcanic belt of Manitoba and system, Saskatchewan-Manitoba; Can. J. Earth Sci., v5, Saskatchewan; Can. J. Earth Sci., v15, p1112-1121 . p1489-1504. Sibbald, T.1.1. (1984): Gold metallogenic studies, Morris, A. (1960): The geology of the Trout Lake area Sulphide Lake area, Saskatchewan; in Summary of (east half), Saskatchewan; Sask. Dep. Miner. Resour., Investigations 1984, Saskatchewan Geological Survey; Rep. 42, 22p. Sask. Energy Mines, Misc. Rep. 84-4, p122.

Simpson, F. (1975): Surficial deposits of the lie-a-la ____ (1961): The geology of the Settee Lake crosse (730) and Lac La Ronge (SW 1/4 73P) areas of area (west half), Saskatchewan; Sask. Dep. Miner. central Saskatchewan; Sask. Dep. Miner. Resour., Resour., Rep. 55, 27p. unpubl. rep., 60p.

____ (1962): The geology of the Nistowiak Lake Thomas, D.J. (1984): Geological mapping, Star Lake area (east half), Saskatchewan; Sask. Dep. Miner. area (part of NTS 73P-16 and 74A-1); in Summary of Resour., Rep. 70, 28p. Investigations 1984, Saskatchewan Geological Survey; Sask. Energy Mines, Misc. Rep. 84-4, p21-31 . ____ (1963): The geology of the Trout Lake area (west half), Saskatchewan; Sask. Dep. Miner. Resour., Van Schmus, W.R., Bickford, M.E., Lewry, J.F. and Rep. 77, 22p. Macdonald, R. (1985): U-Pb geochronology of the Trans-Hudson Orogen in northern Saskatchewan, ____ (1965): The geology of the Black Bear Canada; for presentation at International Conference Island Lake area (east half), Saskatchewan; Sask. Dep. on Proterozoic Fold Belts, Darwin, Australia, August, Miner. Resour., Rep. 86, 24p. 1985.

7 Wanless, R.K., Stevens, R.D., Lachance, G.R. and Delabio, R.N.D. (1974): Age determinations and geological studies: K-Ar isotopic ages, Report 12; Geol. Surv. Can., Pap. 74-2, 72p.

Watters, B.R. and Armstrong, R.L. (1985) : Rb-Sr study of metavolcanic rocks from the La Ronge and Flin Flon domains, northern Saskatchewan; Can. J. Earth Sci., v22, p452-463.