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O1986 Government of Ontario Printed in Ontario, Canada

ONTARIO GEOLOGICAL SURVEY Open File Report 5595

Reconnaissance Geology of the Granitic and Gneissic Terranes in the Algoma , Part l by Delio Tortosa 1986

Parts of this publication may be quoted if credit is given. It is recommended that reference to this publication be made in the following form:

Tortosa, Delio 1986: Reconnaissance Geology of the Granitic and Gneissic Terranes in the Algoma District, Part l; Ontario Geological Survey, Open File Report 5595, 121p., 30 figures, 3 tables, and 2 maps in back pocket.

RaoAFontain*

Development GeofQ* Tough Cteoufv Ontario u H Ontario Geological Survey

OPEN FILE REPORT

Open file reports an made available to the public subject to the foDowing conditions:

This report is unedited. Discrepancies may occur for which the Ontario Geological Survey does not assume liability. Recommendations and statements of opinion expressed an those of the author or authors and an not to be construed aa statements of government policy.

Open ffie copies may be nad at the following locations: Mines Library Ontario Ministry of Natural Resources Sth floor, 77 Grenville Street, The office of the Regional or Resident Geologist in whose district the area covered by this report fa located. Handwritten notes and sketches may bo made from this report. Check with the Library or Region- al or Resident Geologist©s office aa to whether than is a copy of this report that may be borrowed. The Library or Ragkuad or Resident Geologist©s office wfll also give you information on copying ar rangements. A copy of this report b available for Inter-Ubrary Loan.

This report la on ffle in the Regional or Resident Geologists©office(s) located at: 875 Queen Street East Sault Ste. Marie, Ontario P6A 2B3

The right to reproduce thk report is reserved by the Ontario Ministry of Natural Resources. Permission for other reproductions must be obtaJiied m writing from the Director, Ctetario Geological Survey.

V/G.Mflne, Director Ontario Geological Survey

iii

FOREWORD

This report represents the first of a three phase reconnaissance geology program which was initiated in 1984 in order to evaluate a number of geological, geophysical, and geochemical anomalies within the granitic and gneissic terranes of the Algoma Region, and to determine whether they represented targets of possible economic interest for follow-up by the mining and exploration community. The report describes the general geology of the area, mineral occurrences, aeromagnetic and geochemical anomalies visited, and provides guidelines and recommendations for further exploration in the area.

V.G. Milne, Director Ontario Geological Survey J y j ABSTRACT A total of 31 aeromagnetic, geochemical, geological, and radiometric anomalies were investigated in the granitic and gneissic terranes in the southern portion of the Algoma District in order to determine whether they represented areas of possible economic interest to the mining and exploration community. Regional airborne radiometric anomalies in the area roughly coincide with the felsic plutonic rocks of the Algoma Plutonic Domain and are the result of potassium-rich granitic rocks and associated radioactive accessory minerals. Above average uranium in lake sediment and water in the Montreal River area and in the Achigan Lake area may be attributed to the presence of underlying felsic plutonic rocks and the occurrence of uranium vein-type mineralization. The aeromagnetic anomalies visited are caused by the presence of a) iron formation- amphibolite, b) diabase-gabbro dikes, c) quartz-magnetite veins and veinlets, and d) magnetite- bearing felsic plutonic rocks and carbonatite. Two types of ©supracrustal© remnants occur in the gneissic areas: a) those consisting of migmatitic, layered, quartzo-feldspathic rocks, and b) those consisting of amphibolite, amphibole-feldspar gneiss, and siliceous metavolcanios. All mineral occurrences visited have a northwest-trending structural control and most are associated with northwest trending, Keweenawan-age, diabase dikes and subordinate lamprophyre dikes. Many of the occurrences are localized at the dike-country rock contact, and are situated in the western portion of the study area. There is an apparently close relationship between northwest trending, linear, positive aeromagnetic anomalies and diabase-gabbro dikes which may provide a useful guide for the delineation of dikes with potential basemetal-silver mineralization.

Vll J

J J

J TABLE OF CONTENTS

page

ABSTRACT INTRODUCTION...... l GEOLOGICAL OVERVIEW...... 3 RESULTS OF FIELD INVESTIGATIONS...... 7 AEROMAGNETIC ANOMALIES...... 7 RADIOMETRIC ANOMALIES...... 9 GEOCHEMICAL ANOMALIES...... 10 METAVOLCANIC-METASEDIMENTARY REMNANTS...... 13 MINERAL OCCURRENCES...... 14 SUMMARY AND DISCUSSION...... 18 RECOMMENDATIONS...... 21 REFERENCES...... 24 APPENDIX A...... 28 J LIST OF FIGURES page Figure 1: Location of Granitic and Gneissic Terranes in the Algoma District, and corresponding project areas..... 2 Figure 2: Location of target areas visited or referred to in the text...... 29 Figure 3: Topographic map showing the location of aeromagnetic anomaly M-l...... 32 Figure 4: Reconnaisance geology and sample locations in the area of aeromagnetic anomaly M-l (after C. Leslie, 1984).. 33 Figure 5: Topographic map showing the location of aeromagnetic anomaly M-3...... 36 Figure 6: Reconnassance geology and sample locations in the area of aeromagnetic anomaly M-3 (after C. Leslie, 1984).. 37 Figure 7: Topographic map showing the location of aeromagnetic anomaly M-4...... 40 Figure 8: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-4...... 41 Figure 9: Detailed geology and sample locations of the magnetite-quartz vein along Highway 556 (M-4)...... 42 Figure 10: Topographic map showing the location of aeromagnetic anomaly M-7...... 45 Figure 11: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-7...... 46 Figure 12: Topographic map showing the location of aeromagnetic anomaly M-8...... 48 Figure 13: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-8...... 49 Figure 14: Topographic map showing the location of aeromagnetic anomaly M-9...... ,...... 51 Figure 15: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-9...... 52 Figure 16: Topographic map showing the location of aeromagnetic anomaly M-ll...... 54 Figure 17: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-ll...... 55 Figure 18: Topographic map showing the location of anomaly M-10..60 Figure 19: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-10...... 61 Figure 20: Topographic map showing the location of aeromagnetic anomaly M-12...... 64 Figure 21: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-12...... 65 Figure 22: Location of radiometric anomalies R-l and R-2; reconnaissance geology across the regional, total count, radiometric anomaly (dashed line)...... 68 Figure 23: Topographic map showing the location of radiometric anomaly R-l...... 69 Figure 24: Reconnaissance geology and sample locations across radiometric anomaly R-l...... 70 Figure 25: Topographic map showing the location of radiometric anomaly R-2...... 72

XI u 1 1 J page Figure 26: Reconnaissance geology and sample locations in the area of radiometric anomaly R-2...... 73 Figure 27: Topographic map showing the approximate location of metavolcanic remnant G-l and aeromagnetic anomaly M-6.. 77 Figure 28: Reconnaissance geology and sample locations in the area of metavolcanic remnant G-l and aeromagnetic anomaly M-6 78 Figure 29: Generalized geology in the Homer Lake area; lined area: layered quartzo-feldspathic gneiss; stippled area: granite and granitic gneisses (after Frarey, 1977)....,,...... 80 Figure 30: Reconnaissance geology and sample locations in the Homer Lake area...... , ...... 81 Figure 31: Reconnaissance geology and sample locations along the Garden Lake Road , west of Homer Lake...... 82 Figure 32: Topographic map snowing the location of the Saymo Lake barite-Pb-Zn occurrence (S-l)...... 85 Figure 33: Reconnaissance geology and sample locations in the area of the Saymo Lake barite-Pb-Zn occurrence (S-l)...... 86 Figure 34: Topographic map showing the location of the Jollineau Pb-Zn-Ag occurrence (S-2)...... 89 Figure 35: Reconnaissance geology in the area of the Jollineau Pb-Zn-Ag occurrence (S-2)...... 90 Figure 36: Topographic map showing the location of the Conway Pb-Zn-Ag occurrence (S-3)...... 93 Figure 37: Reconnaissance geology and sample locations in the area of the Conway Pb-Zn-Ag occurrence (S-3)...... 94 Figure 38: Topographic map showing the location of aeromagnetic anomaly M-2 and the Wolfe Lake Copper occurrence (S-6).. 97 Figure 39: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-2, Wolfe Lake...... 98 Figure 40: Detailed geology and sample locations within trenches of the Wolfe Lake Copper occurrence (S-6)...... 99 Figure 41: Topographic map showing the location of the Camray Uranium occurrence, Theano Point (S-8)...... 102 Figure 42: Detailed geology of the Camray Uranium occurrence showing sample locations (geology after J. Satterly and D. F. Hewitt, 1948)...... 103 Figure 43: Topographic map showing the location of the Ranson Cu-Au occurrence (S-9) showing general geology...... 106 Figure 44: Detailed geology and sample locations in the area of the Ranson Cu-Au occurrence (S-9)...... 107 Figure 45: Topographic map showing the location of the Kristina Copper occurrence (S-10) and reconnaissance geology.... 110 Figure 46: Detailed Geology and Sample Locations in the area of the Kristina Copper Mine (S-10)...... 111 Figure 47: Location map showing geochemical anomalies SSM-1 and SSM-2...... , ...... 114 Figure 48: Reconnaissance geology and sample locations in the area of geochemical anomaly SSM-1...... 115 Figure 49: Topographic map showing the location of geochemical anomaly SSM-2 and the distribution of anomalous elements in lake sediments; see figure 46 for location map. 118 Figure 50: Reconnaissance geology and sample locations in the area of geochemical anomaly SSM-2...... 119

xi 11

LIST OF TABLES

page Table 1: Summary of Deposit and Occurrence Types in the Granitic and Gneissic Terranes, Area 1...... 23

Table 2: Legend and Symbols used for Reconnaissance Geological Mapping...... 30

Table 3: Correlation Coefficients for Geochemical Anomalies SSM-1 and SSM-2...... 120

xv J J Ministry of Northern Development and Mines

Ontario Geological Survey Open File Report #..5595^.

by D. Tortosa 1986

FINANCIAL ASSISTANCE FOR THIS PROGRAM WAS PROVIDED BY THE MINISTRY OF NORTHERN AFFAIRS.

xvi i Li RECONNAISSANCE GEOLOGY OF THE GRANITIC AND GNEISSIC TERRENES IN THE ALGOMA DISTRICT, PART l

INTRODUCTION The reconnaissance geology project was initiated in order to

,, , ,-L ,© © , © © ,,, i © evaluate a number of selected geophysical, geochemical, and © © ; i © j ,. . © : © geological anomalies within the granitic and gneissic terranes in the Sault Ste. Marie Mining Division. The project? area was subdivided into three sub-areas of granitic© " ©©©©"and ©";" gneissic- **T© " ;! rocks (figure 1) : Area l, extends from Sault Ste. Marie east to , and from the north edge of tbe HuronianfSupergroup to the i©. F ; :"!:©. f \ .. ; ;; ©: ;© © "N ,M f Algoma Districtjboundary; Area 2, extends from Mamainse Point to j?: © © Wawa; and Area 3,-i extends from Wawa to Hemlo. © Work started on the project during the latter part of July, with field work focusing on the western half of Area l based out of Ranger Lake, and later out of Sault Ste. Marie. The area is easily accessible by truck and all-terrain-vehicles over secondary roads and bush-roads, and lakes provide further access by boat, canoe, or float plane. Reconnaissance geology was l©© ; © V,; r © : ©l carried-out by the author, assisted by ,E. Haiey who also drafted many of the figures and maps. t © , , .;. ^. - i, .i . . -. Targets to be evaluated were based*© on aeromagnetic,,,i...... and geochemical anomalies defined by previous radiometric,©i !©© -. i- . i-" . -:© -© © ,© -© "-. :i.----.-r, .© ;i f ede r a l and pr o v i n c i a l s u r vey s (f i gu r;S 2, App end i x A). As we 11, a © © number of mineral occurrences and isolated meftavolcanic^ i © i , .. " © © © metasedimentary remnants in the area were evaluated in terms of their geological and metallogenetic significance. c** GRANITIC AND GNEISSIC TERRAIN n V* * It- i|e GREENSTONE BELT *^ *

HURONIAN SUPERGROUP

28 MILBS 40 40 M l l——l KILOMETRES

Figure 1: Location of Granitic and Gneissic Terrains in the Algoma District, and corresponding project areas. Our intention was to establish a better understanding of the geological and mineralization history of the granitic and gneissic terrane which could be useful in the formulation of exploration strategies and thereby assist the private sector in the mineral exploration of the district.

GEOLOGICAL OVERVIEW The granitic and gneissic terranes throughout Area l are indicated on geological compilation map 2419 (Giblin et al., 1974-76) as consisting of unsubdivided granites and migmatites containing small isolated metavolcanic-metasedimentary segments. The rocks are transected by northwest, north-northwest, and northeast trending lineaments and intruded by northwest and north-northwest trending diabase dikes. Two northeast-trending diabase dikes in the eastern part of Area l are apparently displaced by northwest and north-northwest trending lineaments (Map 2). A carbonatite plug (the Seabrook Lake Complex; Parsons, 1961; Thurston et al. 1977; and Sage, 1983j intrudes the granites in the central portion of the area, and has been dated at 1107 and 1109 Ma (K/Ar biotite, Gittenset al. 1967). In a regional geological synthesis of the Central Superior Province, Card (1979) subdivided the area into plutonic and

,, . iv,s. © © © © T ,© } ©©! gneissic domains (Map l, backpocket). Tfre gneissic domains are geologically complex areas consisting of amphibolite, quartzo- i -. , ..-.- i--, . -© .© f~\ , ©© r© feldspathic gneisses, migmatites, and intrusions. The plutonic domains consist of large areas of coarse-grained granite, monzonite, and subordinate granodiorite (Card, 1979). During the course of the field work, boundaries between the granitic and gneissic domains were found to be gradational. The Algoma Plutonic Domain is an area of batholithic proportions which represents the largest area of massive felsic plutonic rock in the ^Jouthern Superior Province (Card, 1979), and has been dated using Rb/Sr (whole rock) and U/Pb (zircon) methods i at ea. 2500-2700 Ma. A }ow Sr87XSr86 ratio indicates little contamination by pre-existing crustal material (Card, 1979). The area is characterized by the presence of anomalously radioactive granitic rocks which exhibit radiometric signatures due to the relative concentration of potash feldspar and radioactive accessory minerals (Charbonneau, 1982). Xenoliths and enclaves of metavolcanics/metasediments and , supracrustal paragneisses occur throughout the Algoma and Ramsey Gneiss Domains which Card. (1979) interprets as forming the ©links© between metavolcanic-metasedimentary belts in this portion of the jfouthern Superior Province. Frarey (1977) outlined! several areas of supracrustal rock in the Algoma Gneiss Domain consisting of partly granitized and migmatized layered quartzo- feldspathic gneisses and amphibolite (G-2, Map 1; Appendix A). He found no evidence of a basement to the metavolcanic - metasedimentary rocks other than tkftte frkeyc ima a marked contrast in the intensity and style of deformation between gneissic rocks and the metavolcanic - metasedimentary belts. As well, he suggested that the northward trend of both the metavolcanic-metasedimen^ary belts and the Huronian Supergroup rocks north of Sault Ste. Marie was possibly due to very early tectonic control. In a regional geolgical study which bordered on the north-central part of Area l, Thurston et al. (1977) identified northwest and north- northwest trending diabase dikes as being the youngest in the area and texturally and petrographycally similar tp the Mackenzie III swarm. The dikes are. characterized by distinct magnetic lineaments which cut across those of the northeast-trending Abitibi swarm. A number ofK/Ar radiometric age determinations indicate that the dikes intruded ea. 1000 Ma (Wanless et al., 1966,1938). Weiblen (1982) in a study of keweenawan intrusive rocks of the Basin foun^l that diabase dikes and sills from around the basin fall into two compositional types: quartz (high-Al) tholeiites and .olivine (high-Ti) thpleiites. Both types are found in the Pukaskwa dike swarm on the north shore of Lake Superior (Bennett and Thurston, 1972), and in the Baraga swarm in Northern Michigan (Weiblen, 198??). Cross-cutting relationships indicate that the quartz tholeiites wer the earliest intrusions. Both compositional types are also found to occur in the Batchewana metavolcanic-metasedimentary belt, i n t r ud i ng maf i c and i nte rmed i at e mejfc ay o l can i c rocks a .1 ong a , northwesterly direction (Grunsky, 1989). A number of Cu-Pb-Zn-Ag occurrences north of Sault Ste. .Marie occupy fracture systems which are closely associated with - northwest-trending diabase dikes (Assessment Files, Sault Ste* Marie District), Pennett( 1,982) after mapping a portion of Hughes : ! © . . C , © © r . .© © J © . © © - © © © -© © © " Township north of,Sault Ste. Marie, concluded that lamprophyre and felsite dikes, and some of the, diabase in the area were of; Keweenawan age, and that there was a close spatial and structural J J association between base metal-silver occurrences and Keweenawan dike rocks. In mapping the Montreal River area, Nuffield (1956) also noted that there was a structural relationship between pitchblende-bearing veins and diabase dikes of Keweenawan age. These dikes apparently fell into two compositional groupings: an older olivine-bearing group and a younger olivine-free group (Lang, 1949). Epithermal, fissure vein deposits of Pb-Zn-Cu-Ag in the Thunder Bay area and in northeastern Minnesota are controlled by fracture systems whiOh are thought to have been active during and after the emplacement of Keweenawan olivine diabase dike swarms in the area (Weiblen, 1982). A lead isotopic study df Pb-Zn-Cu-Ag veins in the Sault Ste. Marie area by Pearson (1960) indicated a probable Keweenawan age for their formation. He interpreted the lead isotopes as reflecting the sporadic formation of mineral deposits over the duration of Keweenawan activity - between 1200-1000 Ma, and that the source of the lead was likely derived from the surrounding Archean granitic rocks. It would appear that Keweenawan tectonic and volcanic activity has played a significant role in the metallogenetic development of at least the western portion of the granitic and gneissic terranes in the Algoma District. The radioactive granites north of the Archean-Huronian unconformity provide an obvious source area for the paleo-placer uranium deposits in the basal Huronian strata (Rbbertson, 1983), ami the metavolcanic- metasedimentary remnants may provide good prospects for base and precious metal deposits. RESULTS OF FIELD INVESTIGATIONS Target areas visited are summarized in Appendix A and located on Maps l and 2 (back pocket) and figure 2. Field work was localized in the western portion of the area because the granitic rocks north of Elliot Lake had been studied previously (Robertson, 1983; Charbonneau, 1982), and a significant number of base and precious metal occurrences were concentrated in the, west.

AEROMAGNETIC ANOMALIES The regional magnetic susceptibility decreases from the granites and gneisses in the north to rocks of the Huronian Supergroup in the south (O.D.M.-G.S.C., 1965; Map 2, backpocket). This change in magnetic susceptibility is generally due to an increase in the thickness of the Huronian sedimentary rock cover. Regional variations in magnetic intensity in the south roughly outline the shape of the Quirk Lake Syncline (6.S.C., 1984). An

l ! intense east-west magnetic low exists over the thickest part of the Huronian section in the and is thought to be the result of pervasive shearing of the Basement rocks along zones of faulting and cataclasis (Card et al., 1984). Regional scale, linear magnetic highs and lows display a pronounced north-northwest trending pattern reflecting the presence of similarly trending diabase dikes and fracture/fault zones (Map 2, backpocket). On a local scale, the causes of positive aeromagnetic anomalies fall into four categories: 1)

- i ; .. ,- , © © l iron formation - amphibolite, 2) diabase-gabbro dikes, 3) quartz- y j magnetite veins and veinlets in granite, and 4) magnetite-bearing felsic plutonic rocks (Giblin and Leahy, 1979) and carbonatite (Parsons, 1961). Four aeromagnetic anomalies north of Ranger Lake ( M-7, M~8, M-9, and M-ll, Map 2; Appendix A) are aligned in a northeast orientation forming a curvilinear continuation of the Iron Formation (M-13). It has been suggested that the magnetic anomalies form a "keel" of folded metavolcanic - amphibolite - iron formation representing the eastern extension of the Batchewana Volcanic Domain (Grunsky, personal communication). The areas of low magnetic susceptibility and relief between magnetic highs represent those areas where the "keel" of the fold belt and associated iron formation has been eroded. The belt of amphibolite-iron formation is in the order of 100-200 metres wide and extends over a distance of about 25 kilometres. Uneroded segments of amphibolite - iron formation are surrounded by granite, granodiorite, and granitic gneiss containing enclaves of amphibolite and amphibole-feldspar gneiss. These are likely associated with the main belt but have been disrupted and separated during granite intrusion and migmatization. In one well-exposed area, amphibolite and iron formation are segmented and intruded by granite and granite pegmatite resulting in an agmatitic nature to the rock (M-8, Appendix A). These segments, although separate, retain their original structural orientation. North-northwest trending diabase-gabbrp dikes containing Fe- Ti oxides display positive linear magnetic anomalies. These dikes

8 appear to occupy fracture systems wfyich are characterized by distinct topographic lineaments exhibiting negative linear magnetic anomalies trending north-northwest (Map 2, back pocket). The dikes are nearly vertical an4 generally between 5 and f 50 metres wide extending from a ^ew hun4red| metres to several kilometres in length. Contacts wJLth the country ropjcs may be sharp or highly sheared and veined with quartz. In the larger dikes the central portion is a medium-to coarse-grained gabbro becoming finer-grained towards the contacts. Mafic minerals are commonly chloritized, and magnetic minerals (Fe-Ti oxides) appear to be evenly disseminated throughout the rock. Magnetite-quartz veins and ve4nlets occur 4n ^e granitic , rocks adjacent to diabase dikes and contribute to the linear positive magnetic anomalies related tq the dikes. Veinlets are usually 1-2 cm thick and 10-100 o^ in length consisting of euhedral magnetite occupying the centre of the vein and subhedral,/ quartz occupying the remainder. Qne particularly large magnet i te?- quartz vein was discovered adjacent and nearly parallel to a north-northwest trending diabase dike along Highway 556 which is associated with aeromagnetic anomaly M-4 (see Appendix A).

RADIOMETRIC ANOMALIES , . ,. : Above average radioactivity ?.n the Algoma District roughly coincides with the occurrence of fels,ic plutonic rocks in the Algoma Plutonic Domain (O. G. S. -G. S. C. , 1979 and G. S...C., 1975; Map l, backpocket). Above average radioactivity centered on the Ranger Lake area reflects the presence of potassium-rich granites J y containing variable proportions of uranium and thorium likely occurring in accessory minerals such as zircon, monazite, and uraninite (R-l and R-2, Map l and Appendix A). The rocks encompassed by the radioactive anomalies consist mostly of orange to pink, medium-to coarse-grained granite with subordinate granodiorite and quartz monzonite. Geological sections and spectrometer readings across radiometric anomalies R-l and R-2 (Appendix A), indicate that the granites generally become more calcic (quartz monzonites and monzonites) away from the radioactive highs. Radioactive granitic rocks from the Ranger Lake area are separated from those north of Elliot Lake by a zone of lower radioactivity which corresponds approximately to the migmatites and gneisses of the Ramsey Gneiss Domain (Map 1). North and east of Elliot Lake, areas of highest radioactivity appear to be segmented by the Flack Lake fault and by a northeast-trending fracture (intruded by diabase). These may represent fundamental crustal fractures which dislocated the plutonic rocks during pre- Huronian time.

GEOCHEMICAL ANOMALIES A large uranium geochemical lake sediment and water anomaly occurs north of Sault Ste. Marie over felsic plutonic rocks of the Algoma Plutonic Domain (O.G.S.-G.S.C., 1979b and Leahy, 1979; anomaly SSM-1, Map l and Appendix A). The rocks consist of leucocratic to mesocratic granite, granodiorite, and subordinate granitic gneiss. The granite and granodiorite are commonly

10 intruded by white feldspar-quartz pegmatite veins which contain visible magnetite and specular hematite. Notably, the area defined by above average uranium in lake sediment also has slightly above average magnetic susceptibility (Map 2, back pocket). As well, the uranium geochemical contours display some continuity with radiometric contours from the Banger Lake area ! ,; . J ..© .i© .; -T © © © -© © J " (Map l, back pocket). These data .along with the above average in situ radiometric readings (anomaly SSM-l, Appendix A)* suggest that the sources of the anomalous uranium in lake water and sediment are the felsic plutonic rocks underlying the area. A second uranium lake sediment geochemical anomaly occurs in the Montreal River area over radioactive granites and numerous pitchblende vein-type occurrences. The geochemical anomaly extends to the northeast parallel to the Montreal River, following the southeast boundary of the Kapuskasing Structural Zone (Map 1). The associated lake water geochemical anomaly, however, is restricted to the immediate area near Lake Superior from Mica Bay to MacGregor Cove, an area characterized by many pitchblende occurrences. The high uranium content in the lake sediments and waters is likely due to the elevated uranium content in the granitoid rocks and also to the uranium occurrences in the Montreal, River area (Priske, 1985,). . .-, ,: l ©© l- P © © - ; " In reviewing the lake sediment and water geochemical data, note was taken of the interpretation of the geochemical data for the north shore of Lake Superior by Friske (1985); work by Sopuck j! . ; © , - © ©- et al. (1980) on a similar survey over the shield area of Saskatchewan; Wolfe (1977) in the Pukaskwa region of Ontario, and

11 Coker (1980) in a geochemical orientation survey in the Montreal River area, Ontario. Sopuck et al., found that copper and uranium ,J in lake sediments have a strong affinity for organic matter whereas zinc, nickel, cobalt, and lead show a strong affinity for -" hydroxide phases. However, Friske (1985) noted that uranium i J concentration in the lake sediments of the Lake Superior area

! reaches a plateau between 2535 and 55SS LOT (loss on ignition). y Wolfe noted a positive correlation between manganese and zinc , (and to a lesser extent cobalt) in stream sediments of the ^ Pukaskwa area which he attributed to co-precipitation with Mn-Fe l oxides, the pH of water, and the bedrock source. For the present i study correlation coefficients were determined for geochemical j anomalies SSM-1 (24 samples) and SSM-2 (15 samples) in order to determine whether physico-chemical environmental parameters might Li be responsible for some of the anomalous values (Table 3, Appendix A). j -j There is a lack of correlation between LOI (loss on ignition) and uranium in the lake sediments for geochemical anomaly SSM-1 J (Appendix A, Table 3) reflecting the 259S to 5536 range in LOI in i the lake sediments and indicating that the elevated uranium J values represent a true reflection of an anomalous source area. In the area outlined by SSM-2 some correlation exists between Fe, "1 Zn, Co, Mo, and Mn (Table 3) which may reflect co-precipitation as Mn-Fe oxide and hydroxide phases; copper shows some positive correlation with LOI reflecting its© preference for organic .J complexes. Therefore some of the above average metal concentrations found in anomaly SSM-2 may be at least partly due "^ to the existing physico-chemical environmental conditions;

12 however, small sulphide occurrences such as ; S-4 (Havilland Bay sulphide occurrence) may also be contributing. A more detailed statistical re-evaluation of the entire sample population is required in order to filter-out those "anomalies" which may simply be due to physico-chemical environmental conditions.

METAVOLCANIC-METASEDIMENTARY REMNANTS Two types of metavolcanic-metasedimentary remnants were investigated during the course of the field work. Those represented by G-l, G-3, and 6-4 (Map 1) consist of metavolcanic and metasedimentary rocks typical of other shield areas; those represented by G-2 (Frarey, 1977) consist of partly migmatized, layered quartzo-feldspathic paragneiss containing minor amphibolite. The enclaves of layered paragneiss are irregularly distributed within the central portion of the Algoma Gneiss Domain whereas the metavolcanic - metasedimentary remnants occur around the perimeter and are oriented parallel to the boundary with the Algoma Plutonic Domain. The more typical metavolcanic-metasedimentary rocks, such as in G-l, consist of grey-green, fine-grained amphibolite, © © ; ©! © .© ..! f" 1 © - © © © © © "! © ainphibole-feldspar gneiss, and siliceous metavolcanic enclosed and intruded by white to pink, medium-to fine-grained granite to monzonite. Another similar remnant (G-3, Map 1) shown as amphibolite gneiss with minor quartz-mica schist on map 2419 (Giblin and Leahy, 1978) occurs 10 kilometers to the east of G-l Based on the present field work, a thin belt of metasedimentary rocks (G-4, Map l) is inferred to occur starting fifteen

13 kilometers west of G-1, and extends over a distance of about 50 as it swings parallel with the Algoma Plutonic/Gneiss Domain boundary to join with the metavolcanic-metasedimentary rocks north of Sault Ste. Marie. The layered paragneisses of G-2 consist of both amphibole- rich and biotite-rich quartzo-feldspathic layers, with the layering defined by variations in the mafic mineral content of the rocks. Layers range from a few millimeters to 4-5 centimetres thick and trend at 110-120 dipping steeply to the north. The boundary to this ©supracrustal segment© is characterized by a change from massive, homogeneous granites and monzonites in the south, through a transition zone of migmatitic and agmatitic rocks, into the layered quartzo-feldspathic gneisses. The agmatite consists of medium to fine grained granodiorite and granite containing segments of mesocratic tonalite, fine- grained granodiorite, amphibole-feldspar gneiss, and amphibolite. Contact relationships between metavolcanic-metasedimentary remnants (G-l, G-3, and G-4) and the granites and gneisses of the Algoma Gneiss Domain are not as well exposed as in the layered paragneisses (G-2). However, agmatite apparently is quite common at the boundary of the Batchewana Volcanic Domain with rocks of the Ramsey Gneiss Domain (Grunsky, 1980), as well as along the northeast trending "keel" of amphibolite-iron formation north of Ranger Lake (14-7,8,9,8611; Map 2).

MINERAL OCCURRENCES All mineral occurrences visited have a northwest trending

14 structural control and most ar^ asspcxiated twith northwest i trending diabase dikes and subordinate lamprophyne dikes. Many U-Fe, Cu-Fe, Pb-Zn-Ag, and some,Fe\\ ©Occurrences are localized at the dike-country rock contact, .within structurally ;preferred sites. Most of the occurrences are found in the western part of the Algoma Plutonic and Gneissic Domains* and there appears to be a change from oxidized assemblages (j.e. hematite - pitchblende - calcite) in the west near the Keweenawan basal unconformity along the shoreline of Lake Superior, to moire re4uced* SJM l phi d e-b ear ing assemblages (ie. cpy-py; ga*-argt-ggnfr; mt-py-fltz) further to the east. Pitchblende occurrences ,in the Montreal: Jiiver area are well documented by Woolverton (1950), Keston C1950), Lang (1949), and Nuffield (1955). In describing the geology of the area Nuffield states: i r .- . . ,, ,-j - . i.© ; : : ! © . ,v -: ©. -, - " Most of the area is underlain by ^granitic intrusive rocks consisting of granite, granite gneiss, and minor syenite, all cut by pegmatite dikes and quartz veins; ,..Keweenawan age rocks are represented by a vast number of diabase dikes, The most numerous and persistent dikes strike we^t tp northwest and dip steeply north. " , . . ;r ,-.:;,-, . .- © ,.. : ,-.., It is at the contacts ofM th^es,e .diabase dikes with the granitic and pegmatitic country rocks that pitchblende-bearing veins are Ipcalized. The mineralization is accompanied by calcitfef and hematite, and the wallrocks adjacent to the veins are orange to red from disseminated hematite for about one metre. The Jollineau Pb-Zn-Ag occurrence (S-2, Map l; j Appendix A);,

15 J which is typical of dike-associated mineral occurrences visited, contact between a northwest trending diabase t is located at the hJ dike and granitic country rocks. The contact area is occupied by i white quartz which together with the diabase has been fractured and sheared along a northwest direction. Fractures in the quartz J near the contact contain both fine and coarse-grained galena, minor pyrite, and calcite; sphalerite was not observed. The l mineralization appears to be limited to fractures in the quartz r rather than the diabase which suggests that fracturing of the *J more competent quartz provided better "ground preparation" and ; , ...... , ... . , ~ - ; - - ,. ... j v .J channel-ways for mineralizing1 solutions. The Conway Pb-Zn-Ag occurrence (S-3) is similar except that the dike rock is a hornblende lamprophyre. The Sill Lake Silver Mine (S-5; producer) and the Jardun Mine (S-7; past producer) are atypical of other J Pb-Zn-Ag occurrences visited in that the mineralization is localized in northwest-trending shear zones which appear to be © either unrelated to Keweenawan intrusive activity (ie. S-5), or have ambiguous geological relationships to Keweenawan dike rocks (ie. S-7). The mineralization in both of these deposits has been ^ dated using Pb/Pb methods as Keweenawan in age (Pearson, I960; Wilson, 1956). The reader is referred to Burns (1956) and - Robinson (1977) for a review of the geology of the Jardun and Sill Lake deposits respectively. Magnetite-quartz-(pyrite) veinlets ranging from 1-2 cm wide ^ and 1CK100 cm in length occur in granitic country rocks adjacent to magnetite-bearing, northwest trending diabase dikes in the area. At a well-exposed rock cut on Highway 556 south of Ranger

16 Lake (M-4, Map 1; Appendix A) a ^QO metre long, vertical, magnetite-quartz- pyrite vein occurs adjacent and parallel to a north-northwest trending diabase dike. The vein is separated from the dike by about 10 metres of granite and is enveloped by a , fractured and brecciated zone about 5 metres wide. Within th|s frature envelope, magnetite fills fractures and forms the matrix to fragments of granite. The quartz-magnetite vein is up to one metre wide and 60 metres long consisting of variable proportions of quartz and magnetite containing small fragments of granite and pink feldspar. Disseminated pyrite is common in samples of massive magnetite, and a small zone of massive pyrite occurs in the northwest end of the body which gave an above average value of 32 ppb gold (background = ^2 ppb). Vein-type copper occurrences such as the Hanson occurrence (S-9), the Wolfe Lake copper occurrence (S-6), and the Kristina -L " - © © © : ! :© - copper mine (S-10), have similar geological characteristics and i j © i . .©© © - ! v© © © . © © - i setting as the uranium and Pb-Ag-Zn showings. In a geological report by G. Stenning for Kristina Copper Mines in 1956 (Assessment Files, Sault Ste. Marie), he writes: " It became very clear during the geological mapping of the property that the ore-bearing structures are related to the faults along which the diabase dikes were intruded. Later northwest faulting parallel to the dikes has given rise to the structures in which the ore bodies were localized. The ore bodies formed in a series of fissures which. ..strike N70W. " He further states that "the main ore zone in shaft #6 Is localized in a shear zone striking northwest and dipping 65 southwest. The

17 copper mineralization occurs in irregular pockets in a quartz vein which appears to have filled openings in the shear zone". l In both the Wolfe Lake and Hanson Copper prospects* copper j mineralization is localized in shear zones at or near the -i diabase/gabbro - country rock contact. In addition, the Hanson iJ occurrence (Chelsey Twp.) contains galena and calcite at its© eastern extremity which suggests that there may be some overlap J between Pb-Ag-Zn and Cu^Fe types of occurrences. J SUMMARY AND DISCUSSION The regional airborne radiometric anomalies (Map 1) roughly ^j coincide with the rocks of the Algoma Plutonic Domain and are the result of K-rich granitic rocks and associated radioactive accessory minerals. A number of geologists including Robertson (1983) support a modified placer origin for the uranium bc l rev 4, deposits in the Elliot Lake area, and Athat the deposits were r\ derived from cratonized Archean terrain (including the radioactive granitic rocks) to the north and northwest. Similarly, the uranium in Keweenawan vein-type deposits of the Montreal River area likely had their source in the enclosing Archean granites and granite pegmatites; the distinction between the two deposit types lies in the development of an oxidizing atmosphere after ea. 2300 Ma ("oxyatmoversion", Roscoe, 1973) and *— the resulting mobility of uranium in solution. Lake sediment and water geochemical uranium anomalies in the ~~ Montreal River area (S-8, Map 1) can be attributed to the presence of felsic plutonic rocks and Keweenawan uranium vein- type occurrences (Coker, 1980; friske, 198IJ5) * In the Achigan Lake area, lake sediment and water geochemical uranium anomalies (SSM- 1, Appendix A) appear to, reflect the presence of radioactive felsic plutonic rocks underlying the area and may also ^f reflect**^ the presence of uranium vein-type.mineralization similar to that at Montreal River. Based on correlation coefficients of a limited geochemical sample population, anomalous metal contents in some lake sediments can be correlated with alpove average iron, manganese, and LO I (loss on ignition). This may reflect cQ-precipitation of basemetals with Mn-Fe oxides antf hydroxides, or scavenging by organic complexes. A detailed statistical re-evaluation of the entire sample population similar to that completed by Sopuck et al. (1980) in the Shield area of Saskatchewan, is required in order to filter-out those ©anomalies© which are due to ; the prevalent physico-chemical environmental cpnditions in the area.t Two types of supracrustal remnants occur in the Algoma Gneiss Domain: in the central part of the Domain the rock enclaves are composed of migmatitic, layered quart; go- f o Idcpath i c gneisses; around the perimeter of the Domain the rock enclaves are composed of metavolcanics and metasediment?! and are,; roughly oriented ^ ; parallel to the Algoma Gneiss/Plutonic Domain boundary jCMap 1). A fairly continuous belt of supracrustal rocks in the western part of the Algoma Gneiss Domain (G-4 f Map 1) can be traced over a distance of about 50 km as it©swings parallel to the Algoma Gneiss Domain boundary td join with the metavolcanic- metasedimentary rocks north of Sault Ste. Marie. Assessment files

19 (Gaudette Twp., Sault Ste. Marie Mining Division, Innes, 1984) J indicate the presence of sulphides associated with muscovite- sericite schist, graphitic schist, and fine-grained paragneiss within the belt, which bear some resemblance to gold-bearing strata in the Hemlo area. The change from oxidized mineral assemblages (ie. hematite - calcite -pitchblende) to reduced mineral assemblages (ie. cpy- py; ga-argt-sph; mt-py-qtz) found with increasing distance from the Keweenawan basal unconformity in mineral occurrences associated with Keweenawan dike rocks is believed to reflect the deeper level of erosion which is exposed east of the Keweenawan unconformity. A change from an oxidized to a reduced assemblage may be explained by a vertical zonation in the types of mineral occurrences which are associated with Keweenawan intrusive dikes. In the near surface or upper crust portion, diabase intrusion gives rise to the circulation of oxidized, surface or near surface water which results in the mobilization and deposition of uranium near the Keweenawan basal unconformity. At deeper levels, dike intrusion results in the circulation of more reduced fluids which mobilize and deposit Pb-Zn-Ag-Cu, resulting in deposits which are not spatially associated with the unconformity. A general geologic history of dike-associated mineral occurrences may be subdivided into four stages: A) The development of large scale northwest-trending fractures in granitic and gneissic country rocks. B) The intrusion of mafic magma along northwest fractures. C) Fracturing and/or shearing along the dike-country rock contact followed by quartz flooding.

20 D) Fracturing, shearing, and brecciatl^Qfc along the dike- quartz-country rock contact-area followed by the formation of mineralized veins in the quartz, dike, and country rock. - i i * A northwest-southeast orientation appears to have been the preferred direction of tectonic dislocation due to the nature of the regional Keweenawan tectonic environment and the presence of early-formed, northwest-trending zones of weakness. The time span between each of these stages was likely not very great, and the mafic magma would have been an important heat source during the early history.

RECOMMENDATIONS Within the granitic and gneissic terranes of the Algoma District Keweenawan-age Pb-Zn-Ag, Cu, and U mineralization exists throughout the western portion of Area l (Table l, Map 1). It is important to emphasize that some of the Pb-Zn-Ag deposits are (were) primarily silver deposits (ie. Jardun and Prace Mines). Some of the copper prospects hosted in quartz veins adjacent to diabase-gabbro dikes such as the Banson Occurrence (S-9), contain significant gold content in grab samples (0.17 oz/ton). Further prospecting is recommended along contacts pf similar northwest and north-northwest trending, diabase dikes and along northwest- trending structural discontinuities and lineaments throughout the western portion of Area 1. As well, deposits such as the Tribag Mine (Cu-porphyry), which is, fi Keweenawan-age diatreme-like breccia intruding the metavolcanic-metasedimentary rocks of the Batchewana Volcanic Domain (Pearson, 1980), may have similar analogues in the granitic and gneissic rocks of the area. It is

21 also important that further study be given to the spatial distribution and lithogeochemistry of Keweenawan dike rocks in order to determine whether there are any characteristics which may be useful in distinguishing between those which are associated with mineralization and those that are not. The apparently close relationship between north-northwest** trending, linear, positive aeromagnetic anomalies and diabase- gabbro dikes may be a useful guide in locating dikes with potential basemetal-silver mineralization. However, many of the Keweenawan dike rocks which have associated mineralization are not highly magnetic and not easily detected on 1:50,000 scale aeromagnetic maps. A higher resolution aeromagnetic survey and/or airborne gradiometer survey over areas of interest would outline dike positions more accurately. Similarly, ground magnetometer surveys could serve as a useful complement to detailed geological ground follow-up in order to establish contact positions and possible associated mineralization. For Part 2 of the Sault Ste. Marie Reconnaissance Geology project, geophysical, geochemical, and geological data available for Area 2 (figure 1) will be evaluated and followed by field investigations of selected anomalies and anomalous areas. This area is of importance because it borders on the Michipicoten metavolcanic^metasedimentary belt which contains many lode gold occurrences and deposits in both the metavolcanics (the Canamax ©New Zone©) and in the adjacent granites and gneisses (Renabie Mine). Table 1: Summary of Deposit and Occurrence Types in the Granitic and Gneissio Terrains, Area l

Age Lithology Element D= deposit Reference in Text Association Q~ occurrence or on Maps l fc 2

PROTEROZOIC Keweenawan Cu D,0 S-4, 6, 10 Igneous Rocks Cu-Au 0 S-9 U D,0 S-8, SSM-K?) ,.. :. ©ii , © © i".©- © " D,0 S-2, 3, 5, 7 Ba-Zn-Pb 0 S-l Fe j 0 M-4 ARCHEAN ©Greenstone© Au 0 G-l, 3, 4 (?) Enclaves Mo 0 G-4 Fe , ,,Q... M-3, 7, 8, 9 M~ll, 12, 13

Granites fc Gneisses U P R-l, 2, 3 Mo-Cu O

23 REFERENCES Bennett, G. and Thurston, P. C. 1972: Operation Pukaskwa, of Algoma and Thunder Bay: Ontario Department of Mines and Northern Affairs, y Open-File Report 5073, part l, 93p. Bennett, G. 1982: 1981 Report of the Sault Ste. Marie Resident Geologist; in Annual Report of the Regional and Resident Geologists 1981, Ontario Geol. Surv., Misc. Paper 101, p.127-138. Burns, R.D. 1956: The Geology of the Jardun Mine, Sault Ste. Marie, Ontario; Unpublished M.Se. Thesis, Michigan College of Mining and Technology, 58p. Card, K.D. 1977: Regional Geological Synthesis, Central Superior Province; in Current Research, Part A, Geol. Surv. Can., Paper 79-1A, p.87-90. Card,K.D., Gupta, V.K., McGrath, P.H., and Grant, F. 1984: The Sudbury Structure: Its Regional Geological and Geophysical Setting; p.25-43 in The Geology and Ore Deposits of the Sudbury Structure, edited by E.G. Pye,A.J. Naldrett, and P.E. Giblin, Ontario Geological Survey, Special Volume l, 603p. Accompanied by Map 2491, at a scale of 1:50,000, Map NL-16/17-AM Sudbury, at a scale of 1:1,000,000, and 3 charts. Charbonneau, B.W. 1982: Radiometric Study of Three Radioactive Granites in the Canadian Shield: Elliot Lake, Ontario; Fort Smith, and Fury and Hecla, N.W.T.; in Uranium in Granites, ed. Y.T. Maurice; Geological Survey of Canada, Paper 81-23, p.91-99. Coker, W. B. 1980: A Geological Orientation Survey for Uranium of the Montreal River Area, District of Algoma, Ontario; Geological Survey of Canada Paper 79-18, 25p. Frarey, M.J. 1977: Geology of the Huronian Belt between Sault Ste. Marie and Blind River, Ontario; Geological Survey of Canada, Memoir 383, 87p. Friske, P.W.B. 1985: Regional Geochemical Reconnaissance: interpretation of data from the north shore of Lake Superior, ; Geological Survey of Canada, Paper 84-21. Geological Survey of Canada 1984: Aeromagnetic Map NL-16/17-AM (coloured), Sudbury, District of Sudbury, Scale: 1:1,000,000.

24 Geological Survey of Canada 1975: Airborne Radioactivity Map with Profiles, Blind River, N.T.S. 41J; O.F.R, 262. Giblin, P.E., Leahy, E.J., and Robertson, J.A. 1974-76: Sault Ste. Marie - Elliot Lake Geological Compilation Series Algoma, Manitolin, and Sudbury Districts, Ont. Geol. Surv., Map 2419. Giblin, P.E. and Leahy, E.J. 1979: 1978 Report of Northeastern Regional Geologist and Sault Ste. Marie Resident Geologist; in Annual Report of the Regional and Resident Geologists, Ontario Geological Survey, Misc. Paper 84, p.89-98. Gittins, J., Maclntyre, R.N., and York D. 1967: The Ages of Carbonatite Complexes in Eastern Canada; Canadian J. Earth Sci., Vol.4, p.651-655. Grunsky, E.G. T 1980: Geology of the Cowie Lake Area, District of Algoma; Ontario Geological Survey Report 192, 67p. Accompanied by Map 2426, scale 1:31,680 (l inoh to l mitle), Innes D.G. ,, f 1984: Highland-Crow Resources, Goulais River Property; Sault Ste. Marie Assessment Files, Gaudette 0024. Keston, N. 1,1 1944: Radioactive Occurrences,, Sault Ste, tor i e Area and Some Considerations Affecting Exploration Practice; Lang, A. H. 1949: The Camray Uranium Discovery; Trans. Canadian Institute Mining and Metallurgy, Vol52, No. 444, P.42-46. Leahy, E.J. 1979: Unpublished Compilation Map of G*odogical, Geochemical, and Radiometric Data and Mineral Occurrences, Sault Ste. Marie, j Resident Geologist©s Office;. Nuffield, E. W. 1955;, Geology of the Montreal River Area; Ontario Department of ^ines, Vol. 64, Part 3, 32p, : O. D. M.-G. S. C. 1965: Aeromagnetic Maps 7068G, 7069G, 7077G, 7078G, Algoma and Sudbury Districts; Ontario Department of Lands and Forest, and the Department of Mines and Technical Surveys. O.G.S.-G.S.C. 1979a: Uranium Reconnaissance Program, Airborne Gamma Ray Spectrometer Survey, Chapleau, N.T.S. 410, Maps 35242G and 36541G with profiles.

25 O.G.S.-G.S.C. 1979b: Regional Lake Sediment and Water Geochemical Reconnaissance Data, Eastern Shore, Lake Superior, Ontario; O.F.R. 5266. i Parsons, G.E. y 1961: Niobium-Bearing Complexes East of Lake Superior; Ontario Dept. Mines GR3, 73p. Accompanied by Maps 2005,2006, \ and 2008, scale l inch to 1/4 mile. ^ Pearson, W.N. l 1980: Copper Metallogeny* North Shore Region bf Lake Huron, Ontario; y Unpublished Ph.D. Thesis, Queen©s University, 403p. -i Robertson J.A. yt 1983: Huronian Geology of the Blind River Uranium Deposits; O.G.S. Open File Report 5430, 159 p. Robinson, D.J. ^ 1977: The Prace Pb-Zn-Ag Deposit; Unpublished B.Se. Thesis, University of Western Ontario, 54p. ,. : © ©.© L* Roscoe, S. M. 1973: The Huronian Supergroup, A Paleoaphebian Sucession Showing Evidence of Atmospheric Evolution; in The Geological Association of Canada Special Paper No. 12, Ed. G.M. Young 1 © p.31-48. Satterly, J. and Hewitt, D.F. i 1948: Report on a Pitchblende Occurrence at Theano Point, Lake Superior, Ontario, Ontario Dept. Mines, Prelim. Report No. P.R.1948-49. ^ Sage, R. P. 1983: Geology of the Seabrook Lake Carbonatite Complex, Ontario Geological Survey, Open File Report 5414, 63 p. k 2 figures, 5 photos, 4 tables, and l map in back pocket. Sopuck, V.J., Lento, D.A.W/, Schreiber; B.T., and Smith J.W.J. ^. 1980a: Uranium and Base Metal Dispersion Studies in "bhe Maguire Lake Area, Saskatchewan, Geology Division, Paper G78-10, 73p. Sopuck, V. J. -, 1980b: Interpretation of Reconnaissance Lake Sediment Data in the Precambrian Shield Area, Saskatchewan; Saskatchewan Research Council, Geology Division, Paper G78-10a, 53p. Stenning, G. 1956: Geological Report Submitted tb the Ontario Department of Mines ^ on behalf of Supercrest Copper Mines Limited; Sault Ste Marie Assessment Files, Laverendrye 00l2-Bl.

26 Thurston P. C., Siragusa, G. M., and Sage R.J*l 1977: Geology of the Chapleau Area, Districts of Algoma, Sudbury, and Cochrane; Ontario Division of Mines, GR157, 293p. Accompanied by Maps 2551 and 2352* scale 1:250,000, and Map 2221, scale l inch to 4 miles (1:253,440). i i' Wanless, R.K, Stevens, R.D., Lachance, G.R., and Rimsaite, J.Y.H. 1966: Age Determinations and Geological Studies^ K^-Ar Isotopic Ages, Report 6; Geol. Surv. Canada, Paper 66-17, lOlp. ; - '-••f ' ©.©©i -i Wanless, R.K. , Stevens, R^D,, Lachance, G.R,, and Edmonds, C.M. 1968: Age Determinations and Geological Studies, K-Ar Isotopic Ages, Report 11; Geol. Surv. Canada, Paper 67-2, Pt.A, 141p. Weiblen, P.W. 1982: Keweenawan Intrusive Igneous Rocks; in Geology and Tectonics of the Lake Superior Basin, Ed. R.J. Wold and W.J. Hinze, p.57-82. Wilson, J.T., Russell, R.P. , and Farquar, R.M. 1956: Economic Significance of Basement Subdivision and Structures in Canada; Can. Iris t. Min. Metal I., Annual Meeting, Quebec City. ! * Wolfe, W.J. 1976: Regional Geochemical Reconnaissance of Archean Metavblcanic- Metasdimentary Belts in the Pukaskwa Region; Ontario Div. Mines, GR 158, 54p. ; Woolverton, R.S. 1950: The Camray Discovery Dike a^d Associated Uranium Deposits; Unpublished M.Se. thesis, MaGill University, 78p.

27 APPENDIX A Target areas visited and/or referred to in the text page LOCATION MAP...... 29 LEGEND AND SYMBOLS TABLE...... 30 AEROMAGNETIC ANOMALIES...... , . 31 M-1: Monzonite to syenodiorite containing magnetite...... 31 M-2: Diabase-gabbro, quartz-magnetite veinlets (see S-6).. 96 M-3: Iron formation, amphibolite...... 35 M-4: Diabase, quartz-magnetite veinlets...... , . 39 * M-5: Magnetite in Quartz monzonite (Map 1; Leahy, 1979)... M-6: Diabase, intermediate volcanic (see G-l)...... 76 M-7: Iron formation, amphibolite...... 44 M-8: Iron formation, amphibolite...... 47 M-9: Mafic to intermediate meta-tuff, iron formation...... 50 M-10: Diabase, quartz-magnet!te vein...... ;...... 59 M-ll: Amphibolite, Iron formation...... 53 M-12: Amphibole-feldspar-quartz gneiss, Iron-formation..... 63 * M-13: Garden River Iron Formation (Map-1, Grunsky, 1980)... RADIOMETRIC ANOMALIES...... 67 R-l: K-feldspar rich granite...... 67 R-2: K-feldspar rich granite...... 71 * R-3: Granite, Elliot lake area (Map l, Charbonneau, 1982).. GEOLOGICAL TARGETS...... 76 G-l: Garden River metavolcandc-metasedimentary segment. . . '. . 76 G-2 : Homer Lake supracrustal segment...... 79 * G-3: Villeneuve metavolcanic-metasedimentary segment (Map 1; Leahy, 1979)...... - * G-4: Goulais River metavolcanic-metasedimentary segment (Map 1; Innes, 1984) MINERAL DEPOSITS AND OCCURRENCES...... 84 S-l: Saymo Lake Barite Occurrence...... 84 S-2: Jollineau Pb-Zn-Ag Occurrence...... 88 S-3: Conway Lake Pb-Zn-Ag Occurrence...... 92 S-4: Haviland Bay Sulphide Occurrence (see SSM-2)...... 117 * S-5: Sill Lake Silver Mines Limited (Map 1)...... S-6: Wolfe Lake Copper Occurrence...... 96 * S-7: Jardun Pb-Zn-Ag Mines Limited (Map 1)...... S-8: Theano Point Uranium Occurrence...... 101 S-9: Ranson Cu-Pb-Au-Ag Occurrence...... 105 S-10: Kristina Copper Occurrence...... 109 GEOCHEMICAL ANOMALIES...... 113 SSM-1: Achigan Lake area...... 113 SSM-2: Stokely Lake area...... 117 * - referred to only in text

23 c •H O •p •o 0)

(Q 01 O) l-i (O •P (D

C -M o x •H 0) •M -P ia o Q) o .c J 4J rg (U TABLE! 2:; Legend knd Symbols uspd for Reconnaissance Geological Mapping LEGEND INTERMEDIATE TO |4AFIC VOLCANICS GRANllie AND RELATED ROCKS l Unsfubdivided 5 Ujasubdivijci^d ia Amphibolite 5a Qbarts Mdhsonite j l b Metabasaft Sb frondhjemite le Plow or Intrusion 5c Granodiorite 5d priorite 5 e Tbnal i t^ Gneiss INTERMEDIATE TO FELSIC JVDLCANICS 5f BorjnfolQnde Monzonite Sg Hornblenae Syenite 2 Unsudivided 5fa; tjybjrid Grieiss 2r Rhyolite 56 Quarts plpjrite 2d Dacite 5 j Granitic Gneiss 2t Felsic to Intermediate Tuff 5y Pegmatite 2x Felsic td Intermediate Breccia i 5m Migmatite Sk Hbijhbleflde Syenodiorite METASEDIMENT& \ 01ABASB3 6 (Jnsiubdivided 3 UnsubdiVided 0m Magnetic 3w Wacke 6n Nonmagnetic 3s Sandstone Porphyritic 3c Conglomerate 3f Iron Formation AND AMPtOPHYRE 3m Mudstone 3t Siltstone 7 b P!^lisi-ke|ffrec(iiia felsite EAftLY MAFIC INfKUSIONS Felsite lampophyre 4 Gabbro 7 c Carbonat^ Lajnprophyre SYMBOLS B ,;: l .. ...^,,©r i, , LJay e rj ing/Foliation ing/Faulting Geological Contact Fracture Outdrop Location i .. ,© ; i- OT-II47 Rock Sample NOTE: TV-1A Spectrometer Readings indicated as: Tl ©-© (in counts per minute) T2 ~ U+Th T3 - Th

30 FIELD REPORT TARGET: Aeromagnetic Anomaly, M-1 AREA: Gros Cap area, east of Sault Ste, Marie TOWNSHIP: Prince Twp. DATE OF FIELD INVESTIGATION: July 5 fc 6, 1984 (by C. Leslie) U.T.M. CO-ORDINATES: North Anomaly 687,400 mE ; 5,160,300 mN South Anomaly 688,400 mE ; 5,156,300 mN MAGNITUDE,© DIMENSION, SHAPE AND ORIENTATION Of ^NOMALY: North Anomaly: y 6-0*, 000 gamma ;isomagnetic contour: Long Axis 4 4500 metres Short AxJ^s ;-r 700 metres Shape ,-^iliptlcai, linear - Oriehtation. © ^Tl©i-V-K-1 ", NW;-: - trend: © . © ; ":? ©; :: South Anomaly: ^ 60,000 gamma Isomagnetic contour: Long 4xis:"|-i ^300 metres Short Axis * 1400 metres Shape - Irregular Orietitatlon * rough Nl^ trend Average magnetic background f 59,600 - 59,700 gammas SPECTROMETER READINGS: (Monzonite) (mafic-rich monzonite) Tl - 1500 c/m Tl s. 1-500 c/m T2 i r 80 c/m T2 ? 120 c/m T31 : = ,©/30 " ©c/m; . " -,; ;: X3 - 50 c/m TOPOGRAPHY OVER ANOMALY: high SAMPLES COLLECTED: CL-8 4-2-4 : Hornblende CL-84-2-2: Hornblende CL-84-j2-7a: Hornblende morikonite CL-84-2-7b; Diabase ; ; x j | CL-84-3-1: H o r n b l^endje in on ^on i t ^ ,r CL -84 -3 -2 : Hornblende monzonite CL-84-3-4- Diabase.,.©""":r©.:© : "--ri.©:""©:.-n. © -, CL-84-3-5: Hornblende syenodiorite fit-84-4-1©: Hornblende monzonite A - Assay: Au,Ag,etc. S - Qualitative Spectrometrib Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis MM Ir! im H H H

,i5ffa^j!S5fiStt PAJKEG^-RAPHfc--t .^..-.. i u. K* -1 l . ' Figure 3: Topographic map showing the location of aeromagnetic anomaly M-l. N

Figure 4: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-l (after C. Leslie, 1984). 33 GENERAL GEOLOGY (condensed from C. Leslie field report) j Geological compilation map 2419 (Giblin et al., 1974-76) indicates that the area is underlain by granitic and migmatitic j rocksX Field examination of the magnetic anomalies by C. Leslie ^ (field notes, 1984) indicated the presence of hornblende syenite, syenodiorite, and hornblende monzonite characterized by a crude . east-west gneissosity. Small diabase dikes in the area trend .J east-west to north-south and are weakly magnetic. An unmineralized shear-zone 25 cm wide transects monzonite at one location and strikes east-west,dippin 30 j north. The magnetic intensity is highest in the hornblende ** syenodiorite and there appears to be a correlation between the mafic content of the rock and its© magnetic susceptibility. w Source of Information O. D. M.-G. S. C. 1963: Sault Stellar i e Sheet, Algoma District; Ontario ta- Department©b-f Mines - Geological Survey of Canada Aeromagnetic Series, Map 2200G, Scale 1:63,360 or l.inch to l mile. Survey flown 1962-1963. ^

J FIELD REPORT TARGET: Aeromagnetic Anomaly, M-3 ABEA: West of Ranger Lake, ; l;;: j V , TOWNSHIP: Hughes Twp. , Jollineau; Twp. © DATE OF FIELD INVESTIGATION: Juli* 17, V1984 (by : C. Leslie) U.T.M. CO-ORDINATES: 292, 100 ffi! ; © J5, 193, 6QO mN i ; © :, -,; ^ MJ i . - ©T-i;.,,,. ",, .

MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION, ©©. ; © © .. OF © ANOMALY:. . . ©i ©"© > 60,000 gamma isomagnetic contour: Long Axis - 1660 met re^ Short Axis -1060 metres Shape - circular to ellipse-shaped Orientation - WNW trend ©:©;-©H ©^ - 1 - 1 - : :v. ; -. . ©.-. Average magnetic background : 59, 600 - 59, 700 gammas SPECTROMETER READINGS: (Amphibolites) ^- ,. (iron formation) Tl -©1500©c/m - Tl r 1500 c/m T2 - 80 c/m , T2 s 120 c/m T3 = 30 c/- T3 ; 2 . 50 c/m TOPOGRAPHY OVER ANOMALY: high relief SAMPLES COLLECTED: :l.; © © ; " - CL-84-4-5-1: Amphibolite) CL-84-4-5-2a: Pyritic shear zone, Au ^. 01 oz/tiAg A CL-84~4-5-2b: Pyritic shear zone x Au x A CL-84-4-5-2c: Quarts vein material Au s A CL-84-4-5-2d: Quartz Vein material : Au - A CL-84-4-5-2e: Quartz vein material Au " A CL^84-4-5-2f : Quartz vein material Au s , CL-84-4-5-3: Banded Iron 1 f oration CL-84-4-5-4: AmphibolitiKj unit GL-84-r4-5-5: Banded i r 6n formation A - Assay: Au,Ag,etc. S - Qualitative Spectrometer i c Analysis WR - Whole Rock Chemical Analysiiif Tr -Trace Element Analysis ft 2000 4000 6000 aeromagnetic Figure 5: Topographic map showing the location of anomaly M-3. 01 d) M (Q . Q) ^ x: oo •M (Tt •H C •H * (U {Q -H C H O (Q •H 0) 4J J (O O * O O

0) tt H 4J Cum E (O fO -^ to m •O l c x (Q

Q) (O O E H O atO toC "o Q) -H O 4J C Q) (O C to en CO 01 rt E (O O C J-i C 0) / O 01 o (D •w f ft O

(D

•H Cb GENERAL GEOLOGY (condensed from C. Leslie field report) The northeastern half of Hughes township was mapped by Bennett (1982) who described the area as underlain mostly by gneissic tonalites and migmatites. The northeast portion of the area is occupied by coarse-grained quarts monzonite containing narrow segments of amphibolite. Numerous diabase dikes and subordinate lamphrophyre and felsite dikes intrude the basement rocks. The aeromagnetic anomaly is localized over a section of amphibolite containing magnetite-rieh bands interlayered with black chert (banded iron formation). The iron formation is likely in the form of a lense causing a localized magnetic anomaly. A rusty shear zone occupies the contact between a northwest trending diabase dike and medium grained monzonite. The shear zone which appears to change into a quartz vein along strike is about 35 metres long and 3 metres wide and contains copper oxides and pyrite.

Source of Information O. D. M.-G,S. C. 1963: Ranger Lake,Sheet, Algoma District; Ontario Department of Mines - Geological Survey of Canada, Aeromagnetic Series, Map 2214G, Scale 1:63,360 or l inch to l mile. Survey flown 1962-1963.

38 FIELD REPORT TARGET: Aeromagnetic Anomaly, M-4 AREA: Ranger Lake Area TOWNSHIP: Reilly Twp. DATE OF FIELD INVESTIGATION: August 8, 1984 U.T.M. CO-ORDINATES: 311,000 mE; 5, 196,000 mN MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF ANOMALY: > 60,000 gamma isomagnetic contour: ! Long Adcis- 2000 metres i Short Axis -250 metres ; Orientation - NW trend Average magnetic background: 59,600 - 59, 700 gammas SPECTROMETER READINGS: General Area (Granite): Over Anomaly (Diabase) Tl s 5500 c/m fi r 1500 c/m T2 s 300 c/m s T2 ^ 100 c/m T3 r 100 c/m r f3 r 20 c/m TOPOGRAPHY OVER ANOMALY: Low ground, Lpw relief SAMPLES COLLECTED:

A, S DT-1000 : small quartz-magnesite/vein in granite DT-1001 : granite DT-1002 : gabbro ©si DT-1003 : granite ^ A, S DT-1004a: large ©quart z-magnet it e vein (1+00 S) A, S DT-1004b: , " * ,.©: . " (2+00 S) A, S DT-1004c: (3+00 S) A, S DT-1004d: (4+00 S) DT-1004e: granite (5+00 S) A, S DT-1004f : diabasje (5+00 S) ^ ^ WR+Tr DT-1004f: diabase (5+00 S) A, S DT-1004g: quartz-magnetite vein in diabase 6+OOS 4 <2 A, S DT-1004h: large iquartg-magnetite vein (3+50 S) 5 ^ A, S DT-1004i: (2+50 S) 3 <2 A. S DT-1004J: r " (1+50 S) A, s - DT-1005 : massive fin^ygrained pyrite in quartz-magnetite vein 32 <2 A - Assay: Au,Ag,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis

39 J J J

yl

y

l ft 4000 6000 Figure 7: Topographic map showing the location of aeromagnetic anomaly M-4.

HO N FIGURE 9 DT I004o* OT 1005

Figure 8: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-4. DT 1005 N

DT J

OT

DTl004b

OT 10041

DT 1004c

DT I004h

DT I004d

QUARTZ MAGNETITE BODY FRACTURE ZONE OT I004a 54-00 DT I004f

A LJ

Figure 9: Detailed geology and sample locations of the magnetite-quartz vein along Highway 556 (M-4). GENERAL GEOLOGY In a regional synthesis of the Central Superior Province, Card (1979) places the area in the "Algoma Plutonic Domain", consisting of massive to foliated felsic plutonic rocks (Map l, back pocket). Reconnaissance geological mapping in the area of the anomaly indicates the presence of massive, medium-grained, pink to red granite which in places is cut by granite pegmatite veins trending at about 140 degrees, dipping vertically. An isolated quartz magnetite vein about one metre long and 15 cm wide occurs in the granite and has a strike of 060 and a vertical dip. No major regional structural features occur in the 1-2 kilometer area around the magnetic! anomaly. Detailed mapping along Highway : 556* parallel to the long axis of the anomaly, indicates the presence, of a northwest trending diabase-gabbro dike cutting medium grained, pink to red granite. The diabase dike is strongly magnetic and about 10-15 metres wide extending over a total exposed length of almost one kilometre. A large, hematized fracture in granite strikes at 350 and dips 70- 80 east and likely forms the west contact of the dike at the south end. At the north end of the, exposed dike,* and separated by 15 metres of granite, is a quartz -magnetite vein 60 metres long and 1-2 metres wide, trending northwest with a vertical dip. The vein is enveloped by a zone of fractured to brecciated granite about 5 metres wide. Magnetite fills fractures and forms the matrix to fragments of granite. The, quartz -magnetite, vein consists of variable proportions of quarts and magnetite containing small fragments of granite, pink feldspar, and quartz. Disseminated pyrite is common in the samples of massive magnetite, and a small zone of massive pyrite (about 30 cm X 15 cm X 5 cm) occurs at the northwest end of the vein which has an above average gold content of 32 ppb ( background ^ The northwest trending aeromagnetic anomaly can be directly related to the northwest trending, magnetic, diabase-gabbro dike which has large and small qua rt z -magnetite veins associated with it. The large northwest trending quartz-magnetite vein may represent the last vestiges of crystallization of the diabase- gabbro dike; a high titanium content preclude.^ it from being remobilized iron formation (Table 1).

Sources of Information O. D. M. -G. S. C. 1963: Mashagama Lake Sheet, Algoma District; Ontario Department of Mines - Geological Survey of Canada, Aeromagnetic Series, Map 2228G, Scale 1:63,360 or l inch to l mile. Survey flown 1962-1963.

43 y FIELD REPORT TARGET: Aeromagnetic Anomaly, M-7 AREA: Ranger Lake Area TOWNSHIP: Me II l Veen twp. DATE OP-FIELD INVESTIGATION: August 10, 1984 U.T.M. CO-ORDINATES: 304,000 mE; 5,209,000 mN MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF ANOMALY: > 60,000 gamma isomagnetic contour: Long Axis - 800 metres Short Axis - 200 metres Shape ©- elliptical Orientation - NE trend Average magnetic background: 59,600 ~ 59,700 gammas SPECTROMETER READINGS: General Area (Granite Gneiss) Over Anomaly (Amphibolite) Tl s 3500 c/m Tl - 2500 c/m T2 = 200 c/m T2 - 100 c/m T3 - 40 c/m T3 - 60 c/m TOPOGRAPHY OVER ANOMALY: Low ground, Low relief SAMPLES COLLECTED: DT-1012 feldspar-quartz-amphibole gneiss DT-1013 sheared diabase, gabbro DT-1014 grahite, poor foliation DT-1015 granite gneiss, coarse-grained A - Assay: Au,Ag,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis

J

44

J

w t. TARGET: Aeromagnetic Anomaly, M-8 AREA: Ranger Lake Area TOWNSHIP: Fine Twp. DATE OF FIELD INVESTIGATION: August 16, 1984 August 17, 1984 U.T. M. CO-ORDINATES: 297,OOP mE; 5,207,000 mN MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF ANOMALtf > 60,000 gamma isomagnetic contour; Long Axis - 1200 metres Short Axis - 500 metres ; Shape - Heart-shaped Orientation - NE trend Average .magnetic ^background: 59,600 - 59,70b gammas SPECTROMETER READINGS; General Area (Migmatite) Over Anomaly (Granite) Tl - 3500 c/m tl * 5500 c/m T2 s 150 c/m T2 ^ 300 c/m T3 - 70 c/m T3 - 100 c/m

TOPOGRAPHY OVER ANOMALY: High elevation^ (hill), Fligh relief SAMPLES COLLECTED: DT-1048 granodiorite , A, S DT-1049 amphibolite-magnetic Auz4 ppb, Cu^73 ppm A, S DT-1050 iron formation Au^55 ppb WR+Tr DT-1051 amphibolite © DT-1052 pegmatite©granite -; DT-1039 amphibolc-feidspar,-9U4rt3 gneiss DT-1040 amph ibole-*fel dsi par-qiiatirt z gn e i s s xen o l i th DT-1041 granddiprite i , DT-1042 granodiorite gneiss* - A - Assay: Au,Cu,etc. S - Qualitative Speotrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis

47 J u •H •P Q) C D* m E O JM O (O M-l O c o •H •M ni o o

0)

01 c •H

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(D i-i 3 O •ri (Q Q) mt4 Q)

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O* •H TARGET: Aeromagnetic Anomaly, M-9 J AREA: Ranger Lake Area, Lac Cherie TOWNSHIP: Nahwegezhic and Pine Twps. DATE OF FIELD INVESTIGATION: August 24, 1984 U.T.M. CO-ORDINATES: 293, 000 mE ; 5, 207..4.-ppO .nty . , l( f U MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF ANOMALY: H > 60,000 gamma isomagnetic contour: y Long Axis - 1600 metres Short Axis - 300 metres M Shape -elliptical-cigar **"* Orientation - NW trend Average magnetic background: 59,600 - 59,700 gammas w . i © i l! TOPOGRAPHY OVER ANOMALY: Hilly, moderate relief © © j:*--* © ] SAMPLES COLLECTED: * "- WR+Tr -DT-1073 : intermediate tuff DT-1074 r granite veins WR+Tr Df^l075 : mafic to intermediate tuff DT-1076 : granitized tuff DT-1077 ^amphibolite L

A - Assay: Au,Ag,etc. S - Qualitative Spectroinetric An&lysis WR - Whole Rock Chemical Analysis ©y T r - Trace Element Analysis c !

50

J y u

(O 0) Ut (O 0) •C 4J

C •H

CO C O •H y 0 X m * •" o a (D - ^ * r\. M "* •^ E m w * Cv •O l x* J c z 03 ^ 5NrH Dt (0 O E •H O 0 C 0 d) (Q O* o - I O 0) -H 0 4J C 0) (0 C m I co 0* CO (0 •H E m m o * C M x 1- 5 I C 0) - - " 1 O tO m x o Q) m a o

d) (M 3 O* •H Pu TARGET; Aeromagnetic Anomaly, M-14 AREA: Gong Lake area, Anvil area ; TOWNSHIP: Handleman-Havrot Twps. DATE OF FIELD INVESTIGATION: October31, 1994 U.T.M. CO-ORDINATES: 312,000 mE ; 5,217,000 mN MAGNITQDE, DIMENSION, SHAPE AND ORIENTATION OF > 60,000 gamma isomagnetic contour: ; Long Axis ^ 8&00 metres Short Axis -1000 metres Shape - linear, irregular Orientation - NE trend r Average magnetic background: 59,600 - 59,700 gammas TOPOGRAPHY OVER ANOMALY: elevated ground, high relief SAMPLES COLLECTED: i © " -" '.- f j DT-1183 : Diabase ,l DT-1184 : Amphibole-feldspatf gneiss A - Assay: Au,Ag,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis f \ GENERAL GEOLOGY IN THE VICINITY OF TH| ANOMALIES M~7, M-8, M-9, M-ll On the geological compilation inap 2419 for the Sault: Ste. Marie -Elliot Lake area, Giblin e-fc ak (1974-76),! show the rocks in this area as granitic in composition, containing minor amounts of migmatite and© iron formation, t^e magnetic anomalies occur near t hie boundary between the "Ramsay Gneiss^ Domain" and the "Algoma1 Plutonic Domain" of the CentraV Superior Province (Card, 1979), Thj3se four magnetic anomalies ^re aligned in a northeast orientation foiling a curvilinear oon^inuat f on of t^ie Goulais River ae^rpmagnetic anomaly (M-13j caused by the Goulais River : iron fofm&tion), It has been suggested that!these magnetic anomalies^ represent the "keel" to the foldeel amphibolite-iron , formation on the eastern extension 6f the Batchewana Volcanic Domain (Grunsky, personal communication, 1984). A regional northeast-^trending lineament ocdurs just a few hundred metres to the northwest of the anomalies and parallels the rock-domain boundary.

53 y u

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0) rHa Em . tn .-i r-i T3 l c x (Q ^ 5* .H en to o E ^H o o c 9 id en u (U -H O 4J B O) (O C (O CD oi ra •H E ffi O c u C (U O (Q U0) IM a o

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GEOLOGY OVER THE ANOMALIES jj Anomaly M-7 : i * Traverses parallel to and cutting across the magnetic anomaly y indicate the presence of a northeast trending, approximately 100 metre wilds area of amphibolite and amphibole-feldspar gneiss with j* moderate! magnetic susceptibility, locally containing thin-bedded y sections of magnetiifee-chert invaded by granite veins and extending over several metres of exposed outcrop. The amphibolite , and amphibole-feldspar gneiss contain cross-cutting granite l pegmatite veins from a few centimetres up to one metre in width. Small pods and lenses of chlorite and/or epidote, 3 to 6 centimetres in size, occur concordant with the foliation in the j j amphibolite. Some of these pods appear to be the product of M extreme isoclinal folding resulting in a very thick hinge zone with veity thin, pinching limbs. l , i North and south of the© metavolcanic-metasedimentary.. belt y the rocks consist of granitic to monzonitic gneisses, foliated 5 granite, and a quartz-feldspar-amphibole-biotite gneiss with the j foliatipn striking at about 240. A small zone of breccia about 10 Ul metres in diameter encountered in the granitic gneisses consists of about one-half metre size, light green, aphanitic, felsic ! fragments contained in a white quartz matrix. The f^.ne-grained L fragments resemble ©felsite©. The granitic gneisses contain widely scattered segments of amphibolite which are quite likely related to the main belt, but have been disrupted and separated during migmatization. The granitic gnetisses have also locally ^ undergone nearly contemporaneous intrusion of both aplite and pegmatite dikes during a period of brittle fracture. North- j northwest trending diabase-gabbro dikes crosscut all the rock L- types in the area. Anomaly M-8: ^ Three traverses were completed in the area of the anomaly; on a road traverse putting across the strike extension of the i isomagnetic {60,000 gamma) contour, the rocks are predominantly ~~ migmatites and agmatites consisting of amphibole-feldspar gneiss and amphibolite xenoliths contained in a white, medium-grained \ (in places pegmatitic), granodiorite groundmass. Some xenoliths consist of crudely foliated granodiorite to diorite gneiss containing pink feldspar porphyroerysts, 1-2 cm in size. All the , rocks are cut by a northwest trending diabase-gabbro dike about ^j 75 metres wide.

56 Northeast of the road and following the long axis of the magnetic anomaly, a small hill was found to consist of granite and quarts monzonite containing isolated segments of lineated amphibole-feldspar-quartz gneiss. Further to the northeast a second hill with good outcrop exposure cbnsists predominantly of medium grained to pegmatitic quartz-feldspar granite containing large segments of amphibolite and banded iron formation. Segments of amphibolite are magnetic, trending in an 6agt-northeast direction, and are separated ffom segmented iron formation by a zone pegmatitic granite. The banded iron formation consists of 1- 2 cm thick beds of interlayered grey quartz and magnetite, the elongate segments of amphibolite and iron formation can vary in size from less than a metre up to 10-20 metres long and 1-2 metres wide, and are intruded by granitic veins resulting in an ©agmatitic© character to the rock. Anomaly M-9: A lake-shore traverse across the axis of, ,the magnetic anomaly indicated the presence of a zone of thinly laminated, fine grained metavolcanics containing approximately equal proportions of quartz, feldspar, and mafic minerals and could be ,classified as an intermediate meta-tuff. The layering in the rocks has a strike of 325 and a dip which can vary from 45 to 90. Small open folds in the rock plunge at 20 to the east and give tjhe rock the appearance of a crenulated schist. The meta-tuff is intruded by cross-cutting granitic veins. Bounding the metavolcanic zone are granitic and migmatitic rocks. In places, the meta tuff has been partly "granitized" leaving only vague relics of the laminated texture in a rock which now consists of mostly fine-grained pink feldspar and quartz. On the north side of the metasedimentary zone a large section of fine-grained, poorly foliated to non-foliated, siliceous mafic metavolcanic is intruded by granitic veins which are offset by small northeast trending faults resulting in a left hand strike displacement of about one-half metre. The highest magnetic susceptibility occurs within the area of the meta-tuffs, however these rocks were found to be only slightly magnetic. The rock exposure along the shore is good, but the likely source of the magnetic anomaly is overburden covered and is likely caused by a small area of iron formation.

57 Anomaly M-ll: t M A geological reconnaissance in the area indicated the presence of a northeast-trending ^one of amphibolite and amphibole-feldspar gneiss Qir&c-tly underlying the magnetic i-, anomaly. The amphibotit^ and amphibole-feldspar gneiss are surrounded on either si4^ by granitic rock, and intruded by a : , slightly magnetic diiibaS^-fabbro dike. Contacts of the y supracrustal sone with the surrounding country rocks are covered by overburden as is the location of iron formation. t M Sources of Information O.D.M.-G.S.C. U 1963: Goulais Lake Sheet, Algoma District; Ontario Department of Mines - Geological Survey of Canada, Aeromagnetic Series, Map 2215G, 1:63,360 or l inch to l mile. y Survey flown 1962-1963. O. D. M.-G. S. C. 1963: Marisea Lake Sheet, Algoma District; Ontario Department ^ of Mines -Geological Survey of Canada, Aeromagnetic Series/Map 2229G, Scale 1:63,360* or l inch to l mile. Survey flown 1962-1963. ^

53 FIELD REPORT TARGET: Aeromagnetic Anomaly, M-10 ; AREA: Ranger Lake Area TOWNSHIP: Reilly Twp. DATE OF FIELD INVESTIGATION: August 11, 1984 U./T.M. CO-ORDINATES: 306,000 mE ; 5,204,000 mN ! MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF ANOMALY: > 60,000 gamma isomagnetic contour: Long Axis - 3^00 m&t^es - Short Axis - 1000 metres Shape - ellipse pinched at the ends Orientation --NW 1?rend Average magnetic background: j59*600 - 69,700 gammas SPECTROMETER READINGS: . General Area (Granite): Over Anomaly (Diabase): TT s 8000 c/m " Tl ^ 1500 c/m M T2 - 400 c/m , ; T2 i 76 c/m T3 s 150 c/m ^ T3 = 60 c/m TOPOGRAPHY OVER ANOMALY: high ground, rolling hills SAMPLES COLLECTED: .,,J - DT-1016A : Granite DT-1017 : Granite WR+Tr DT-1018 : Diabase , T

A - Assay: Au,Ag,etc. S - Qualitative Spi^ctrometr i c Analysis \ WR - Whole Rock Cheilical Analysris , ; Tr - Trace Element Analysis s

59 y j y j A) Q) h (O

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(U 14 o*3 •H b* GENERAL GEOLOGY , j J i On O.G.S. Map 2419 (Geological Compilation Series, Sault Ste. ^ Marie - Elliot Lake Area, Giblin et al. 1974-76), show the rocks in the area of the anomaly as granite. In a regional synthesis of i the central Superior Province K. Card (1979) places the area in ^ the "Algoma Plutonic Domain", consisting of massive to foliated felsic plutonic rocks (Map l, backpocket). Reconnaissance ; j geological mapping in tne area of the anonialy indicates the y presence of massive, medium-grained, pink to red granite. No major regional structural features occur in the 1-2 kilometer . area around the magnetic anomaly. M East^west and north-south traverses over the anomaly indicate the presence of borthwest trending diabase dikes with a high \ magnetic susceptibility, intruding medium to coarse-grained Ll granite which has a strong airborne radiometric signature (see radiometric anomaly R-2). Small veinlets of quartz-magnetite , j occur in the granite adjacent to magnetite-beading diabase. A y large diabase-gabbro dike 50-60 metres thick and exposed over about a l km strike length appears to be the main cause of the aeromagnetic anomaly. ! aeromagnetic anomaly M- l O and the associated diabase dike may bte the northwest continuation of the magnetite-bearing diabase dike (anomaly M-4) which occurs south of Ranger Lake and has a large magnetite-quartz vein associated with it. Similar size magnetite-quartz veins may not be exposed around M- 10 due to the extensive overburden cover.

Sources of Information O. D. M. -G. S. C. 1963: Ranger Lake Sheet, Algoma District; Ontario Department of Mines - Geqlogical Survey of Canada, Aeromagnetic Series, Map 2214G, Scale l inch to l mile. Survey flown 1962-1963. FIELD REPORT ~: TARGET: Aeromagnetic Anomaly, M-12 AREA: Gong Lake Area TOWNSHIP: Hoffman Twp. DATE OF FIELD INVESTIGATION: August ©17, 1984 ; U, T. M. CO-ORDINATES: 303,000 mE ; 5,222,000 mtf MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF ANOMALY: > 60,000 gamma isomagnetic contour: Long Axis ^ 9Qp*metres Short Axis - 3^0 metres Shape - Elongate heart-shape Orientatio^ -- E*W trend Average magnetic background: 59,600 - 59,700 gammas SPECTROMETER READINGS: General Area (Tonalite gneiss) Tl s' 1500 T2 - 10O * T3 - 60 TOPOGRAPHY OVER ANOMALY: Hill SAMPLES COLLECTED: DT-1043: tonalite DT-1044: Iron formatidn-amphibolite^pegmatite DT-1045: Tonalite gneiss DT-1046: Amphibole-fe|dsp^r gneiss WR+Tr DT-1047: Gabbr0-diabaie . ~ Assay: Au,Ag,etc. , f v"*; - Qualitative Spectrometric Analysis - Whole Rock Chemical Analysis - Trace Element Analyst^ , GENERAL GEOLOGY ^ : " s i-,. j i "© © . - ' On geological compilation map 2419 for the Sault Ste. Marie - Elliot Lake area Giblin et al. (1974-76) shov the rocks in the area of the anomaly as consisting mostly ofvunsubdivided granites and mig^matl©tes witjh isolated sections 5f iron formation. In a regional synthesis of the central Superior Province K. Card (1979) places the area in the "Riimsey Gneiss JDoroain" (Map l, backpocket). No major regional strUQtural features occur within the immediate area around the magnetic anomalyi

63 J y

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L i Figure 21: Reconnaissance geology and sample locations in the area c aeromagnetic anomaly M-12. 65" lil J

North-south traverses across the anomaly indicate,the j presence of leucocratic medium-grained amphibole-feldspar-quartz gneissconsisting of about 20-50& amphibole, 40-7C^ white feldspar, and less tlffan 10% quartz. The rock can be classified as j a tonalite gneiss witti the darker amph i bole-rich bands defining a ~*~* crude layering and foliation trending 280. In some outcrops the rock moderately magnetic. A small, apparently isolated segment of i iron formation occurs within the tonalite gneiss and is intruded aJ by a quartz-feldspar pegmatitic vein. Presumably, larger sections of iron formation are responsible for the size and shape of the j aeromagnetic anomaly but are hidden by extensive overburden J cover. A large body of diabase-gabbro with moderate magnetic susceptibility occurs at the eastern end of the magnetic anomaly and may contribute to the overall magnetic pattern in the area. j Sources of Information l O. D. M.-G. S. C. .j- 1963: Goulais Lake Sheet, Algoma Districtj Ontario Department of Mines - Geological Survey of Canada, Aeromagnetic Series, i©Map"©221 SG, Scale 1:63,360 or l inch to l mile. Survey flown 1962-1963. FIELD REPORT TARGET: Aiborne Radiometric Anomaly R-i AREA: Mashagama Lake Area ; TOWNSHIP: Renwick-Rollins twp. V" DATE OF FIELD INVESTIGATION: August 21, 1984 U.T.M. CO-ORDINATES: 323, 000 mE©; 5, 198, 000 mil MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF THE ANOMALY: > 3 eU Radiometric cohtouz*: Long Axis - 6000 metres j ©Short Axis "v- 1^00 metres Shape -elliptical Orientation ~ E-W trend SPECTROMETER READINGS: General Area Over Anomaly; (Diabase) : (Granodiorite-Quartz Monebnite) (Granite-Quartz Monzonite) Tl = 8500 c/m Tl - 10000 c/m iT2 - 450 b/m i T2 ^ 500 e/m T3 - 80 c/m -: T3 - 100 c/m TOPOGRAPHY OVER ANOMALY: Higher elevation thatn surrounding area. SAMPLES COLLECTED: DT-1006 Radioactive Later ed gneiss DT-1007 Granite DT-1008 Granite WR+Tr DT-1009 Quartz Monzonite DT-1010 Granite DT-1011 Granite + magnetite-quart? veinlet DT-1032 granodiorite to quartz monzonite WR, Tr DT-1054 DT-1055 quartz monzonite A, S DT-1056 quartz ^-magnetite vein, Au ppb, Ag <2 ppm DT-1057 granite WR+Tr DT-1058 granite, quartz monzonite DT-1059 granite DT-1060 granodiorite WR+Tr DT-1061 granite A Assay: Au,Ag,etc, S Qualitative Spectrometric Analysis WR Whole Rock Chemical Analysis Tr Trace Element Analysis oO* ^^ c m m 6 vi o ffi C

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Figure 24: Reconnaissance geology and sample locations across radiometric anomaly R-l. TARGET: Aifeorne Radiometric Anomaly R-2 ^ AREA: Saymo Lake Area TOWNSHIP: Reilly and Mcilveen Twps. DATE OF FIELD INVESTIGATION: August 12, 1984 U.T.M. CO-ORDINATES: 307/000 mE ; ,i 5,205,,000©© mN MAGNITUDE, DIMENSION, SHAPE AND ORIENTATION OF THE ANOMALY: > 2600 ops (total) Radiometric contour: Long Axis ~- 6500 metres Short Axis - 6500 metres Shape -circular. ^ Orientation -N/A ,, SPECTROMETER READINGS: f ;. , f General Area Over Anomaly (Diabase): (Granodibrite-Quartz Monzonite) (Granites-Quartz Monzonite) Tl r 7000 c/m Tl 3.© 9000 c/m T2 = 300 c/m T2 = 400 c/m T3 s 60 c/m T3 ~ 50 c/m TOPOGRAPHY OVER ANOMALY: Higher el^ya^ion than surrounding area, SAMPLES COLLECTED: WR+Tr DT-1019 granite. DT-1020 diabase, gabbro DT-1021 A, S DT-1022 Quarts Vein in granite, Au X2 ppb, Ag ^ ppm WR+Tr DT-1023 Diabase, Gabbro ; A, S DT-1024 Barite-quartz~scheejite vein, Ag <0. l oz/t DT-1025 Quart ^ itton^Qpite DT-1026 Diabage, Gabbro^ DT-J027 Granitie DT-1028 Gpanodioritja, quartz monzonite WB+Tr DT-1029 Diorite DT-1030 Granite - WR+Tr DT-1031 Diabase DT-1032 Granocliorite " A - Assay: Au,Ag,etc.. S ;- Qualitative ^Spectrometeritf Analysis WJR - Whole Rook Chemical Analysis Tr - Trace Element Analysis

71

i/a Ml 3 MILKS

KM KILOMETRES

Figure 26: Reconnaissance geology and sample locations in the area of radiometric anomaly R-2. GENERAL GEOLOGY IN THE VICJHITY OF THE ANOMALIES: j On Geological Compilation Map 24J43 for the Sault Ste. Marie - Elliot Lake Area Giblin art al,| (3^74-76), show the rocks in the area of anomaly R-1 and R-2 as consisting of granite with minor l ammounts of quartz monzonite and trondhjemite. The radiometric l- anomalies occur in an area of radioactivity which centers around the Ranger Lake area and constutdtes one of three regional radiometric anomalies occurring in . :tihe ©Algoma Plutonic Domain© ^ (Card, 1979; Map l, backpocket). The other two regional anomalies occur north of Elliot Lake, and Hiave been studied by Charbonneau ; (1982) in a comparison and evaluation of radioactive granites in -i the Canadian Shield. The highest radioactivity in the ganger Lake regional anomaly is centered on Mashagama and Sayrao Lakes (RI and R3;j respectively, : figure 1). The high integral opui|t for the Mashaganfrfi Lake area ul (3000-4000 ops) reflects high uranium and pot as s i uni counts (> 3 eU ppm and > 2 eK % respectively); in the Saymo Lake area the , high integral count reflects high uranium counts (©^ 3 eU ppm). ^ North-south traverses were completed in !the Mashagama Lake and Saymo Lake area and along Highway 129 through the eastern portion of the regional radiometric anomaly. The rocks -^ encompassed by the anomalies consist mostly of orange to pink, medium-grained, granite with lesser ammounts df granodiorite and quartz monzonite. The traverse on Highway 129 cuts through the ^ eastern, lower radioactive portion of the regional radiometric anomaly and encompasses monzonites and quartz monzonites in places becoming porphyritic with K-feldspar phenocrysts. Past the northern limit of the regional athomaly the rock is a white, ~~ medium-grained granodiorite containing biotite. A notable characteristic of/tfee Saymo Lake area, and less so with the Mashagama Lake area, is 1^he widespread intrusion of northwest-trending diabase-gabbro,©dikes ^ranging in width from about l up to 50 metres, and occurring with a frequency of about ^ one large dike every 500 metres. In mps^ places the dikes are pristine but some of the smaller ones dre sheared, chlqritized, and contain quartz veins which are disposed parallel and ©en echelon 1 to the dike contacts. "~* Based on the radio-element Ratios and the equivalent element concentrations, the Saymo Lake anomaly is likely due to an above average uranium content in the rocks in the form of accessory minerals such as sircon and uraninite and partly due to the presence of potassium-rich granite. In the Mashagaina Lake area the radiometric values indicate that the anomaly is due to both a high uranium and potassium consent In the rock reflecting predominantly the presence of uraniferous potassium-rich granites. Both areas area characterized by potassium-rich granites which become more calcic (quartz monzonite and monzonite) away from the radiometric highs.

Sources of Information O. G. S.-G. S. C. 1979: Uranium Reconnaissance Program, Airborne Gamma Ray Spectrometer Survey, Chapleau, NTS 410, Maps 35242G and 36541G with profiles. Geological Survey of Canada 1975: Airborne Radioactivity Maps and Profiles, Blind River, NTS 41J; Open File Report 262.

75 FIELD REPORT © i TARGET: Garden River Metavocanic-metasedimentary Remnant, G-l ! AREA: Ranger Lake Area w TOWNSHIP: Snow/Cuthbertson Twps. DATE OF FIELD IfrVESTiGATION: August 17, 1984 U.T.M. CO-ORDINATES: 303,000 mE ; 5,222,000 mN ~- SPECTROMETER READINGS: y Metavocanios/metasediments Granites: Tl = 2000 c/m Tli: 5000 c/m T2 s 150 c/m T2= 300 c/m J T3 s 50 c/m T3= 60 c/m M SAMPLES COLLECTED: DT-1033: Amphibole-feldspar gneiss WR-i-Tr DT-1034: Intermediate Volcanic ! WR-fTr DT-1035: Amphibolite jj DT-1036: Diabase-Gabbro DT-1037: Granite DT-1038: Diabase Ml A - Assay: Au,Ag,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis v- Tr - Trace Element Analysis GENERAL GEOLOGY ^ On geological compilation map 2419 for the Sault Ste. Marie - Elliot Lake area, (Giblin et al. 1974-76) show the metavolcanic- rnetasediroentary remnant as occurring within urisubdivided granitic rocks of the "Algoma Plutonic Domain" (Card, 1979). Northeast and northwest trending lineaments occur near the area. The best exposure of the metavolcanic/metasedimentary rocks occurs along a secondary road accessible from Highway 556 south of Ranger Lake. The consist of gray-green, fine-grained amphibolite; a grey-green, siliceous, intermediate volcanic; and -J amphibole-feldspar gneiss which exhibits fine layering. The rocks generally strike at 170 with near vertical dip. " Granitic country rocks are white to pink, medium-to fine grained, with a 2:1 ratio of white to pink feldspar. Granitic pegmatite dikes striking E-W intrude the granitic country rocks. ^ At one location, granite and pegmatite intrude amphibolite along ~" a 300 degree bearing. The amphibolite near the contact does not exhibit any indication of contact metamorphism or metasomatic effects. An aeromagnetic anomaly (M-6) is localised over a small ** area covered by overburden and may be due to the presence of diabase.

J

76 Figure 27: Topographic map showing ,tj}e .approximate location of "greenstone©© remnant G-l and aeromagnetic anmfiy M-6. Figure 28: Reconnaissance geology and sample locatidniT in the area of ^greenstone*remnant G-l and aeromagnetic anomaly M-b. FIELDS REPORT TARGET: Homer Lake Suprcrustal Segpent, G-2 AREA: Homer Lake Area TOWNSHIP: Shingwaukonce Twp. W. - DA©EE OF FIELD INVESTIGATION4: August 17, 1984 U, T;; M. CO-ORDINATES: 306,000 mE ; 5, 17,1; 000- mN SMPLES COLLECTED: DT-1134: Diabase with sulphides DT-1135: DT-113@a: Layered 4uatftzo*feldspathic gneiss DT-1136b: Layered quartzo^feldqpat|iio gneiss DT-1137: Quartzo-feldspathic ^neiSs DT-1138a: Monzonite to granodiorite DT-1138b; diorite to gabbro \ DT-1139: Layered qiAartzo-f-eldspathic jgneiss WR-fTr DT-1140: Diabase -t- sulph^desr DT-1141: Layered, gneiss t migmatitje ,, A, S DT-1142: Quartz-chlprite j , Au - 3 ,,ppb DT-1143: Diorite-torialite: gqeiss DT-1144: Layered gneiss,].., " , DT-1145a: Layered gneiss l . ; ©S "©/© , DT-ll45b: Layered gneiss y - r ^ DT-1159: Granite :© ©~- -; v t DT-1160: Metasedimen^^ -f granite i, DT-1161: Layered grifelss © ;- t ) "l DT-1162: Layered gneiss ; " ^ ^; *: DT-1163: Diabase © X ^ w DT-1164: Layered quartzo-feldspathic gneiss DT-1165: Layered quartzo-feldspathic gneiss DT-1166: Diabase :- DT-1167: Quartzo-feldspathic rock DT-1168: Gabbro -*- feldspar pegmatite DT-1169: Layered gneiss DT-1170: Layered gneiss r . DT-1171: Diabase A - Assay: Au,Ag,etc. , S - Qualitative Spectrometric Analysis© WR - Whole Rock C hemical Analysis Tr * Trace Element Analysis © KANE TWP

111! or nit pj.iisaA,t,c

Ml i MILES

KM l HHHhT KILOMCTRES

Figure 29: Generalized Geology in the Homer Lake area; Stippled: layered quartzo-feldspathic gneiss; Asterisks: granite and granitic gneisses; (after Frarey, 1977). to l—'—'^ \ 0 ^^

Figure 30: Reconnaissance geology and sample locations in the Homer Lake area. N

DT 11430 OT 1l45b

UJ

Figure 31: Reconnaissance geology and sample locations along the Garden Lake Road , west of Homer Lake. GENERAL GEOLOGY According to the geological compilation map 2419 for the Sault Ste. Marie - Elliot Lake area (Giblin et al. 197.4-76), the area centered on Homer Lake is underlain by unsubdivided mafic to intermediate volcanic rocks representing remnants of a metavolcanic-metasedimentary belt enclosed by granitic and migmatitic rocks. Frarey (1977) mapped the area 8MS a "large amphibolite mass....fine to medium grained, moderately to strongly foliated, and commonly banded by varying mafic content or by intercalations of pink and grey quartzo-feldspathic material. Small areas of plagioclase-quartz-biotite paragneiss and schist also occur but are seldom large enough to map separately." A road traverse cutting across the strike of the rocks indicated an apparent change from massive, homogeneous granites and monzonites in the south, rfchrqugft a transition zone of migmatitic and agmatitic rocks, into layered quartso-feldspathic gneisses with a variable mafic mineral content..The agmatite consists of medium to fine grained granodiorite and granite containing segments of mesocraitic tonalite, finer grained granodiorite, and segments of anjphibQ^e-feldspar gneiss and amphibolite. In some of the quartzo-feldspathic segments the layering displays complex, small scale folding. The boundaries between the felsic fragments and s the matrix are difficult, to establish in some places. The youngest rocks are quartso- feldspathic, medium-to coarse-grained, veins and dikes. The layered gneisses consist of both amphibole-rich and biotite-rich quartzo-feldspathic layers, with the layering defined by variations in the( mafic mineral content of the rocks. Layers range from a few millimeters to 4-5 centimetres thick and trend at 290-300 dipping steeply to ^jhe north. Some of the quartzo-feldspathic layers are very qoarse grained with a poorly defined foliation resulting in a migmatitic rock. The layered gneisses bepome mafic poor towards the northern edge of the supracrustal segment, appearing more massive and less well- layered. Throughout the beljb the rocfcs are cut by numerous pegmatite arid Aplite dikes and veins which occur parallel to and cross-cutting the foliation/layering. Some of the rock layers may be classified as amphibolite, but the use of the general term 'amphibolite' for the supracrustal belt is misleading. A more appropriate term for these rocks would be 'layered quartzo-feldspathic gneisses'. No obvious large sections of mafic metavolcanic rocks were identified in the area.

83 y y

FIELD REPORT TARGET: Saymo Lake Barite-Pb-Zn Occurrence, S-l AREA: Saymo Lake TOWNSHIP: Mcilveen Twp. DATE OF FIELD INVESTIGATION: August 22, 1984 U.T.M. CO-ORDINATES: 309,000 mE ; 5,205,600 mN SAMPLES COLLECTED: A,S DT-1024: Barite vein Ag *:0.l oz/ton WR+Tr DT-1061: Diabase, east side DT-1063: Quartz adjacent to barite vein DT-1064: Quartz, central part of vein DT-1065: Diabase fragment within barite vein WR+Tr DT-1066: Diabase fragment within quarts vein DT-1067: Quartz vein, west contact with dike DT-1068: Granite DT-1069: Quartz vein boulders DT-1070: Quartz vein contact with granite DT-1071: Granite at southeast contact with vein DT-1072: Diabase at northeast contact with vein A ~ Assay: Ag,Au,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis GENERAL GEOLOGY: Geological compilation map 2419 for the Sault Ste. Marie - Elliot Lake area (Giblin et al. 1974-76) indicates that the area is underlain by unsubdivided quartzo-feldspathic rocks of the "Algoma Plutonic Domain" (Card, 1979). On the main island in the central part of Saymo Lake, a one metre wide quartz vein was discovered by D. Tortosa during the course of the field work. It occurs at the northwest contact of a diabase dike which intrudes the granite country rocks. The diabase dike is part of a larger dike, about 100 metres wide, which can be trace across the island by its characteristically high relief.

34 ft 4000 6000 Figure 32: Topographic map showing the location of the Saymo Lake barite-Pb-Zn occurrence (S-l). (Q ^gj W' * * (D Ui ** * CO* (O 6ft

c •H •H 1 Ul CO •^^ LJ C 0 Q) •H U x x x x x •P C (0 Q) y 5 x x xtn x O 14 8 x x k x x O U( fH 3 * * - ~* U 0) U * * -H a O E c m N (Q 1

T3 S04 c 1 (0 0) 4J w ^ •H W M DI ^ i J HI Q (0 JQ

s! 0) 1o 1CP^: jt (0 C (U J] w O •i N™ C O ra E (Q ^ CQ ra * •H w m c 0) c .c o 4-* u (U m ft 0 o •* ro O I CO 0) ^ I 3 ][ 1 1 D •H b ^~-i. ~s] S K The quartz vein is exposed over a distance of 3-4 metres and displays fracturing in a northwest .direction parallel to the contacts. Elongate diabase fragments,are distributed throughout the quartz vein with the long axis of fragments parallel to the vein walls and the fracture direction. The fragments appear to be well chloritized. The northeast diabase-quartz contact is occupied by a 5-10 cm thick barite vein which contains small fragments of diabase, low-iron sphalerite, calcite, and galena. The quartz adjacent to the barite vein is euhedral and vuggy, containing bits of chalcopyrite and pyrite. On the northwest side of the island the diabase-granite contact is also occupied by a similar type of quartz vein, but no barite or sulphides were found. This might have been due to the lack of good exposure in the area.

o t FIELD REPORT y TARGET: Jollineau Pb-Zn-Ag Occurrence, S-2 AREA: Southwest of Ranger Lake y TOWNSHIP: Jollineau Twp. DATE OF FIELD INVESTIGATION: September 20, 1984 U.T.M. CO-ORDINATES: 298,900 mE ; 5,189,800 mN SAMPLES COLLECTED: DT-1116 Galena Au=32 ppb, Ag^8. oa/ton, ppm DT-1117a: Granite WR+Tr DT-1117b: Diabase DT-1117c: Quartzite DT-1118 : Sheared diabase DT-1119a: Diabase DT-1119b: Galena DT-1119c: Quartzite DT-1120 : Granodiorite and some granite DT-1121 : Granite A - Assay: Au,Ag,Cu,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis PREVIOUS WORK: The occurrence was discovered and staked in 1905. It was later restaked in 1926 by Ranger Lake Mining Company Limited who sunk a shaft to 10 meters. In 1947 and 1948, Sault Lead-Zinc Mines Limited carried-out geological mapping and diamond drilling; and in 1951 Crowshore Patricia Gold Mines did further drilling. In 1966 Briar Court Mines Limited completed a magnetometer survey and 19 diamond drill holes (Assessment Files, Sault Ste. Marie Mining Division). GENERAL GEOLOGY: The occurrence is located at the southwest contact between a northwest trending diabase dike and the granitic country rocks. The contact is occupied by white quarts which together with the diabase has been fractured and sheared in a northwest direction. Pyrite and galena occur within fractures and along shear surfaces. l ft 2000 4000 6000 Figure 34: Topographic map showing the location of the Jollineau Pb-Zn-Ag occurrence (S-2). J j J

26 .5 nil. j—* km.

DT-MI7a 5 V littMhj ^ •'.'./i I J n-r 11111. onus U I1I8

5 l ^7 ii i vein li DT-III9B

fractured qtz i ft

Figure 35: Reconnaissance geology in the area of the Jollineau Pb-Zn-Ag occurrence (S-2). The quartz vein is composed of massive grey to white quarts which is fractured and mineralized near the diabase boundary, but becomes less fractured and grades into the surrounding granitic rooks. Diabase is intensely sheared and chloritized, and locally brecciated. Although some calcite is present on shear surfaces and in fractures in the diabase, no sulphide minerals were found. Fractures in the quartz and near the quarts-diabase contact contain sections of both fine-grained galena and coarse-grained, subhedral to euhedral galena; sphalerite was not seen. Veins tend to be 1-3 cm thick and extend over .a*, short distance ( < 30 cm ). Although quartz is abundant in. the area where mineralisation exists, it is not directly related to the ore and gangue minerals. The mineralization appears, tp be limited td fractures in the quartz rather than ttye diabase which suggests that fracturing of the more competent quarts provided better "ground preparation" and channel-ways for mineralising solutions. The country rocks which the di&e intrudes consist of pink granite and white granodiorite. At one location, not related to the occurrence, the granite is cut by a small fracture zone striking at 305 with a vertical dip; some of the fractures contain hematite and magnetite. Other magnetite-rich veinlets like these may be partly responsible for the above average magnetic susceptibility in the area.

91 FIELD REPORT TARGET: Conway Pb-Zn-Ag Occurrence, S-3 AREA: West of Ranger Lake TOWNSHIP: Hughes Twp. DATE OF FIELD INVESTIGATION: November 14, 1984 U.T.M. GO-ORDINATES: 290,500 mE ; 5,194,300 mN SAMPLES COLLECTED: DT-1190: Lamprophyre DT-1191: Lamprophyre with carbonate veins DT-1192: Sheared Lamprophyre A,S DT-1193: Layered gneisses Au = 11 ppb, Cu - 140 ppm DT-1194: Granitic and migmatitic rock DT-1195: Fine-grained, black rock from shear zone A - Assay: Au,Ag,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis PREVIOUS WORK: The occurrence was discovered in 1926 by J.Conway, and in 1027 St. Regis Lead Mines Limited carried-out stripping, trenching and completed two test pits. In 1949 St. Regis Lead Mines Limited drilled the prospect. Sampling and surface exploration programs were completed by Argoma Uranium Mines Limited in 1955, and in 1970 Polex Mines Limited completed a geological evaluation of the occurrence and recommended further work (Assessment Files, Sault Ste. Marie Mining Division). The present owner is Elsadon Explorations Limited of Sault Ste. Marie. GENERAL GEOLOGY: Previous examination of the area by Bennett (1932) indicated the presence gneissic tonalite and migmatite underlying most of the area. A wedge-shaped section of coarse-grained monzonite containing segments of amphibolite occurs south and east of the Conway occurrence. Diabase dikes are the most common rock type, accompanied by subordinate lamprophyre and felsite. The Pb-Ag-Zn showing occurs in a shear zone which follows the contact between a northwest trending lamprophyre dike and metasedimentary and granitic country rocks. According to an assessment file report on the property by Larable (1956), mineralisation could be traced by pits and trenches over a distance of about 100 metres. During the present study, the pits contained water and no obvious galena was seen in the sheared contact rock. The shear zone consists of sheared lamprophyre which is now a chlorite schist. Most of the contact area forms a topographic low and is overburden covered. a ft 2000 4000 6000 Figure 36: Topographic map showing the location of the Conway Pb-Zn-Ag occurrence (S-3). - - J y

ul l y M: y Km 0

outcrop

DTT119Q \U*-DT-HI4,0T-IIM

m 20

Figure 37: Reconnaissance geology and sample locations in the area of the Conway Pb-Zn-Ag occurrence (S-3).

©fi The rocks adjacent to the lamprophyre dike consists of layered felsic and mafic metasediments trending 265, dipping 70 south which are intruded by granitic veins and masses. The mafic metaseaiments contain disseminated sulphides (mostly pyrite); the felsic metasediments are white, fine-grained and thinly layered, containing a white mica (muscovite). They appear to be of felsic volcaniclastic origin. Chilled mafic dikes up to one metre thick intrude the metasediments parallel to the layering Bennett (1982) concluded that there was a close spatial association between base-metal occurrences in the area and dike rocks of Keweenawan age, and that the dikes and deposits shared fracture systems which were active during Keweenawan time. As well, Lamble (1956) stressed the close association between Pb~Ag mineralisation and the,presence of diabase throughout the area. y FIELD REPORT TARGET: Wolfe Lake Copper Occurrence, S-6 AREA: Wolfe Lake TOWNSHIP i Tupper Twp. y DATE OF FIELD INVESTIGATION: September 21, 1984 U.T.M. CO-ORDINATES: 711,000 mE ; 5,194,500 mN SAMPLES COLLECTED: y Au Cu A, S DT-1122: Hematitic quarts 4- diss. pyrite < 2 ppb 366 ppm A DT-1123: Gabbro 4 quartz, sulphides (cpy) 2 ppb 270 ppm DT-1124: Gabbro 4- sulphides DT-1125: Siliceous Gabbro, diss. pyrite l 1 WR+Tr DT-1126: Gabbro 4- magnetite, pyrite y DT-1127a: Massive quarts DT-1127b Altered granitic rock with magnetite-quarts vein A DT-1127c: Mineralised quarts Au < 2 ppb, Cu ^ 725 ppm WR+Tr DT-1127d: Sheared gabbro, contains phenorysts of pyrite DT-1127e: Mineralised amphibole-mica schist DT-1127f Fine-grained Magnetite WR+Tr DT-1127g: Mineralised and chloritised amphibolite u DT-1127h Mineralised quarts 4 chloritised amphibolite DT-1128: Non-magnetic diabase-gabbro DT-1129: Medium-to fine grained granitic ruck DT-1130: Quartzo-feldspathic rauk,, possibly cataclastic A - Assay: Au,Ag,etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis PREVIOUS WORK: During 1955 and 1956, Pitch-Ore Uranium Mines Limited completed magnetometer and scintillometer surveys, several trenches and 25 diamond drill holes in the mineralized sone. Airborne magnetic, radiometric and electromagnetic surveys were completed over the area in 1956 by Technical Mining Consultants Limited (Assessment Files, Sault Ste. Marie Mining Division). GENERAL GEOLOGY: On geological compilation map 2419 for the Sault Ste. Marie - Elliot Lake area. Giblin et al. (1974-76) indicate that the area is underlain by unsubdivided quartso-feldspathic rocks of the "Algoma Plutonic Domain" (Card, 1979). Some of the quartao- feldspathic rocks in the Wolfe Lake area have a ''proto- cataclastic' texture as indicated by fractured pink feldspar grains and granulated quarts.

y o to E O C (O o •H Jp 0) C IBD* ~** E vo O l M W 0)^ to IH o(D O C Q) C M O M •H 3 •P O 8fO 0U H h o) a0) jc•p oa o- 0 C Q) •rt J-J 3 (d O J .c (O Q) (H 0,1-f m o E S U 0 •rt JC JS -P wa -o ..O*h Cfl acM P ' EH Z

00

(D y y uli N Li u LJ

DT 11270 -Q

KILOMETRES

Figure 39: Reconnaissance geology and sample locations in the area of aeromagnetic anomaly M-2, Wolfe Lake,

Several, tfenches expose a west-northwest trending shear zone M which cuts through-a medium-to coarse grained gabbro intruding j* medium-tb fine grained rooks of granitic composition. The portion of the shear-zoneiKhieh cuts the gabbro is an : ill-defined zone l (partly du© td poor, exposure) which is about ^0 metres wide ^~- consisting of vuggy*, orange sections of quartz containing biotite and chloritized amphibole separated by sections of gabbro and j n siliceous gabbro. Chalcopyrite and pyrite occur as grains y disseminated within the gabbro, in the quarts, and associated with chloritized and hematized amphibolite or altered and sheared f r gabbro. li The portion of the shear-sone cutting quartso-feldspathic rocks is well exposed on the shoreline and consists of a west- f northwest trending, 10-15 metre wide zone of chloritised ^ amphibole and mica schist cut by quartz veins which occur parallel and 'en echelon' to the direction of shearing. The j j contacts of the shear zone are not sharply defined; quarts and y ehloritised amphibolite grade into a quarts-rich rock and then to a pink-orange unfoliated rock (similar to the quartzo-feldspathic country rock). The quartzo-feldspathic country rock appears to have undergone silicification near the shear zone boundaries. ^ Both quartz veins and sheared gabbro are magnetic in places due to the presence of magnetite. Thin ; veins of very fine- LJ grained, grey material occurring within the shear zone exhibit a strong magnetic susceptibility. The unsheared gabbro in the area is also highly magnetic. On aeromagnetic map 2214 the mineral occurrence, shear-sone, and gabbro are characterised by a west- ~" northwest trending, elliptically-shaped area of above average *-' magnetic susceptibility about 800m long and 300m wide. A more general west-northwest trending aeromagnetic anomaly can be — traced from the western end of Wolfe Lake nothwest for a distance of about 8 kilometres. This suggests that the gabbro encountered near the copper occurrence is part* of,a large west-northwest — trending diabase-gabbro dike cutting through the area.

100 FIELD REPORT TARGET: Theano Point Uranium Occurrence, S-et AREA: Lake Superior shoreline^ Spu1:h of Montreal River TOWNSHIP: Slater Twp. DATE OF FIELD INVESTIGATION: November 6, 1984 . ..,, .- ^ U.T.M. CO-ORDINATES: 730,500 mE ; 5,227,800 mN SAMPLES COLLECTED: A; S DT-1185: Mineralized sample, south contact, U-1840 ppm f' DT-1186: Diabase WR-fTr DT-1187:.--.-Coarse-grained pegmatite A, S, DT-1188: Pitchblende vein * altered wallrock, 11=6150 ppm WR+Tr ; DT-1189: Diabase, central part of dike A '- Assay: U, Au, Ag, etc. S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis, Tr - Trace Element Analysis PREVIOUS WORK: , ;, " j The occurrence was discovered in 1847 by J.L. Le Conte and staked in 1948 by R. Campbell ;jlh^ 1949, geological surveys/ trenching and diamond drilling was done by Carnray Mines Limited, and an inclined shaft was sUnk and a level established at 138 feet (Assessment Files, Sault Ste. Marie Mining Divisien). In 1950 development work ceased. GENERAL GEOLOGY: The geology of this uranium occurrence is well documented by Woolverton (1950), Keston (1950), and Lang (1949). The geology of Slater township was mapped|4 by Nuffield (1955) at a scale of l"-1/2 mile. In describing th^ kep|logy Of the area Nuffield states: " Most of the area is underlain by,^ranitic intrusive rocks consisting of granite, gr4^i|te gneis's, and minor syenite, all cut by pegmatite dikes and quarts veins.'/. Keweanawan age rocks are represented by a vast numhe|* of diabase dikes. The most numerous and persistent dikes strike?1 j^est to northwest and dip steeply north. " It is at the contacts of thes;3 diabase dikes with the granitic and pegmatitic country rocks that pitchblende- bearing veins are localised. The mineralisation is accompanied by calcite and hematite. Wallrocks adjacent to the veins are orange to red from disseminated hematite for about one metre.

101 u J

- yl l j y

Figure 41: Topographic map showing the location of the Camray Uranium occurrence, Theano Point (S-8) •p •p **M nt *H** L hi U* |S t- K CO) M 1- -H X lil ^ ~ C -S 0 . n S .C b W 1 go C TJ d) c ui ra i-i •^n 1^1Vi -0 H U Ui 0 0 r O 0) •p E -P I 3 ra L ^ w ra2 - I JH ^ . D r ^ ^0) ra 4J s1 M tu IL— . m. s ra fc " 5*W 1^1 D* 0) O JC rH •P 0 (U 4-1 D)

o* c Ho -H-o O V 4) (O O) Di O UJ V) O OC h- T? H UJ D UJ (D H J H 0) O Z flj Cb 00 -M E ^ ra o* o S (O r-t - UJ 111 UJ Z Q. UJ ^ O (0 t- UJ * " UJ O -J Q) O) < OD M m t O I 3 o: z CP UJ < •ri > o: 5 l Du o o o: o. D UOIH3dnS 3M VI y J

There is a striking similarity in geological setting", * mineralogy, and alteration between vein-type uranium occurrences of Keweenawan age in the Montreal River area along the shore of Lake Superior, and those in the Beaverlodge area on the north U shore of Lake Athabasca, Saskatchewan. Botli areas are- characterized by the presence of continental elastics with j * intercalated Volcanics unconformably overlying granites, granite y gneisses, ahd metasediments. ^Mylonitization followed by late fracturing and brecciation dominates in the Beaverlodge area with , j the uranium deposits associated with major fault systems in y subsidiary fractures and faults close to the major unconformity. Ih the Montreal River area uranium occurrences are more closely related to fractures systems which were active after the intrusion of diabase, during the ''Lake Superior Rifting Event', in areas close to the Keweenawan7basement unconformity. The difference between Beaverlodge and the Montreal River area appears to lie in the size of the fracture systems. The uranium mineralization of late-Proterosoic time occurs in much sinaller fracture systems that are closely associated with diabase dike-country rock contacts; large areas of mylonitization arid brittle fracture are completely absent and accounts for the lack of a well-•developed plumbing system and larger-size uranium deposits.

104 FIELD REPORT TARGET: Ranson Copper Occurrence* S-9~- AREA: Northeast of Echo Lake , 1 TOWNSHIP: Chelsey Twp. DATE OF FIELD INVESTIGATION; October 23, 1984 U.T.M. ;CO~ORDINATES: 274, 500 mS ; 5, 173,250 mN SAMPLES COLLECTED:

A, S DT-1172: Quartz*calcite vein 95 12 11.495 204 DT-1173: Diorite . WR+Tr DT-1174: Diabase' :: DT-1175: Granite Gneiss ? DT-1176: Sheared diabase t- quartz A,S DT-1177: Mineralised vein B760 33 6.7* DT-1178: Sheared Diabafek A, S DT-1179: Mliheralise^ samples 95 7 4.533b 16 DT-118Q: Gabbro-diabase A,S DT-1181: Vein Material 1670 2 134 DT-1132: Gabbro A - Assay: Au,Ag,Cu,etc. , S - Qualitative Spectrometrio Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis ' PREVIOUS WORK: Between 1901 and 1903 three shafts were sunk by Ranson Copper Mining Company Limited to 213, 75, and 47 feet respe/^tively,. In .1947 Glenrock Gold Mines aquired the property and carried-out some bulk sampling of the mineralization and recommended drilling ancj further prospecting. In 1974 Middle River Mines completed l three diamond drill holes, and in 1984 J. Haugeneder completed one drill hole and a trench (Assessment files. Sault Ste. Marie Mining Division) GENERAL GEOLOGY: i-. -l-' r: ' ' ,. ' , Three nnain trenches separated by about 250-300 metres expose a wes t-tnorth wes t trending shear s6n^ ! dlpping 65 north. The! sfcear aon0 oocUrs at or- n^ar the contact between a west-northweSt trending diabase dipping 65 north and the granitic and gneissic country roolts of the area. The mineralisation consists of pyrite, chalcopyrite, galena, and calcite which occur in quarts veins

105 J y o* d) o * JC .H '(p •M O H 0) O c oto •H •* C w*-* o c at to o i M •H to a) +J *- TJ ' to q c u D < o o u C 0) (O (U c-l -H Eb -H a d Q E u •p m u C D* en o O) C E -H •O s* D) C C O W -H a a O Z a (O ^ o 0] Q) < -H o M -4 e E fa o o o z 0Q) SO) 4)

•H O .H •Hto JC-P .Han -P •M *w oE m3 S o u to

O* •H occupying west-northwest fractures in sheared diabase. The shear y zone with the accompanying quarts veins appear to extend over a distance of about one kilometre. During past exploration three diamond drill holes were placed to intersect the diabase, shear ! zone, and accompanying quartz veins and mineralisation. Drill *-* logs indicate that shear zones exist adjacent to both contacts of the diabase, however, exploration concentrated on the better exposed southern contact. y In the eastern most trench a quartz vein, about one metre thick, occupies the contact between diabase and syenodioritic country rocks; shearing of the contact rocks is riot obvious. Chalcopyritej, pyrite, and galena occur mostly associated with caljcite within the quarts vein. The quartz also contains small fragments of! very fine-grained, chloritised diabase. Further to ** the west, on the main showing, mineralization consists mbstly of chalcopyrite and pyrite occurring in quarts veins containing l subordinate calcite. The quarts veins, which occur approximately J 10^15 metres above the footwall diabase contact, occupy west- northwest, trending fractures in sheared diabase. The diabase at an4 above the contact is extensively sheared. Further towards the west the vein size and shearing intensity appear to diminish and -^ 'horsetail' fractures appear in the granitic country rocks, trending southwesterly and containing minor pyrite and chalcopyrite with moderate gold values (1650 ppb). —, Changes in the lithologies which the quarts veins transect seem tp be accompanied by variations in the accompanying mineral assemblage (ie. Cu-Pb-Ag at the diabase/syenodiorite contact to Cu-Fe Vithin ttye diabase). This may have significance in terms of the gold and silver potential if a mineral zonation exists along i strike or down dip. -* The sporadic occurrence of quartz veins along strike and down dip makes it difficult to delineate any mineralized zone without ^j a great deal of closely spaced drilling. A magnetometer survey to better define the diabase contacts followed by detailed overburden sampling and geochemical analysis for copper, sine, lead, silver, and gold may result in tht^ delineation of ~" mineralised zones and provide justification for further work. TARGET: Kristina Cqpper Occurrence,^g-10 ' AREA:, East of Achigan Lake " ^J;, TOWNSHIP; La Verendrye Twp. Jfe; :- DATE OF FIELD INVESTIGATION: October 11, 1984 U.Tr^M. CO-ORDINATES: 722, 5QO mE ; ' 5, 196, 400 mN SAMPLES COLLECTED: s ; - ^ DT-1146: Green (Lorrainf) Quartzite WRfTr CJT-1147: Amphibole-rich Lamprophyre DT-1148: Aplite A DT-1149: Quartz-cpy~py mineralisation,, Au-1520 ppb, Cu~4. DT-1150: Amphibolite 4 * ^ ^ .; , DT-1151; Quartz-cpy mineralisation l DT-1152: Lorrairi (?) Quartzite ,, DT-1153: Lorrain (?) quartsitdl contact area DT-1154: Lorrain (?) quartzite contact area

~ T" -' * ; -(f ' i ,- A - Assay: Au.Ag, etc. , * "l 1 "'' 1 S - Qualitative Spectrometric Analysis WR - Whole Rock Chemical Analysis Tr - Trace Element Analysis - PREVIOUS WORK: ,; :r - : Between 1901 and 1907 Superior d6pper T Company Limited sunk six shafts on the property with most development and production focused on shaft #6. Copper production during this period was 296 tonnes. From 1952 to 1955 KristS,na bbpper Mines Limited completed 31 diamond drill holes and a g"eologi6fal survey. In 1958-57 Supercrest Copper Mines Limited completed geological and geophysical surveys; and 34 di&piond drill holes (Assessment i- Files, Sault Ste. Marie Mining Division). GENERAL GEOLOGY: Geological mapping in the areajcgf' tfte'Kristina Mine by , Roberts in 1941 (Sault Ste. Marie Assessment File: Laverendrye t-0012/Bl) indicated the presence of a large mafic igneous body abo,ut 150 metres wide intruding the granite and granodiorite ccjuntry rocks along a northwester 13^:' d|d reot i on. The igneous mass varies in composition from diorite to diabase .an4 amphiboli5-rich| jamprophyre. The Cu-bearing quarts veins occur at the northeast contact of the intrusive. An outcrop of lamprophyre near the main shaft (#6) is composed mostly of very coarse-grained amphibole \ which is transacted by aplite veins'from 2 cm upto one metre wide trending northeast and northwest. J

J in

•II OUTCROP

*N| QUARTZ

7h| LAMPROPHYRE

6RANITE 'AILIN Of DT-M49 SHAFT DT-II50 N

FT

KfiNO- 3

Figure 46: Detailed Geology and Sample Locations in the area of the Kristina Copper Deposit (S-10); Geology after Superior Copper COmpany Limited, Assessment File Laverendrye 0012-B1. Sault Ste. Marie Mining Division •i ' 1 J

In a geological report by Mr. G. Stenning for Kristina Copper l Mines in 1956 (Sault Ste. Marie Assessment Files), he writes: " It became very cleat* during the geological mapping of the property that the 6re-bearing structures are related to the *-J faults along which the: diabase dikes were intruded. Later northwest faulting parallel toj the dikes has given rise to the t j structures in which the ore bodies were localised. The ore bodies y formed in a series of fissures which...strike N70W." He further states that "the main ore zone in shaft #6 is localized in a shear sone striking northwest and dipping 65 southwest. The M copfer mineralization occurs in irregi^lar pockets in a quarts vein which appears to have filled openings in the shear sone. The hangingwall is frozen to the vein, and there appears to be a j considerable amount of silicification of the wallrock. On the W footwall, the vein is fairly sharp and easy to trace, being limited by a narrow shear zone. No silicification or sulphide dissemination was seen in the footwall of the vein." ^

.i. J. FIELD REPORT TARGETr Geochemical Anomaly, SSM-1 AREA: Achigan Lake area, north of Wabos TOWNSHIP: Marne Twp. DATE OF FIELD INVESTIGATION: September 10, 1984 U. T, M. ; CO-ORDINATES: 713,500 mE ; 5,200,000 i DIMENSION, SHAPE AND ORIENTATION OF ANOMALY: Uranium in sediment Contour: ppm U Length: 24ikni Width: 10 km Orientation: NE-SW trend ' Shape: Irregular, elongate ^TOPOGRAPHY OVER ANOMALY: moderate relief SAMPLES COLLECTED: ::,:,--- -, ,^ ; v- 1" -" i DT-1084: Granodiorite DT-1085: Granite ;,,, * DT-1086: Granite Gneiss WR+Tr DT-1087a: Granite " /,' DT-1087b: Granodiorite - v DT-1088: Qranodiorite - DT-1089: granite : Df-1090: Granite pegmatite /S DT-1090a: Quartz vein ? Au ^ 12 ppb, Ag: X 2 ppb DT-1091: Hornblende qusiYts monsonite : A Assay: Au,Ag,ete. f i j ; S Qualitative Spectrometric .Analysis/ \ WR Whole Rock Chemical Analysis Tr Trace Element Analysis K : READINC5S Average Granite: Average granodiorite Tl^ 6000 ' Tl- 2500 T2^ 350 T2^ 150 ' "' 13- 100 T3r 60 ENERAL GEOLOGY a^rea is underlain predomlij^nf'ly by granodiorite, granite, and a 'granitid gneiss J .;The granitic .gneiss? l* orange-red, medium-grained,; consisting of. henliatize^. porphyroclasts of rounded to elliptical -Shaped feldspars of variable s ise wrapped in chloritised tjiobibe defining a gn^iKsocity in the rock.

113 .. ~ -. o ~ .333 ^ J e e xi e t. O. O. Q. S K o. o. o. T 0-0 li. Ml TJ l b C (D o3 e* "O XH l V CM z fs. ial H-o w o. 01 to 0) •ri e 3 rH •- o flj •o •o E tt O U) O) C ro jj sj xU U 4 O J rt O i M 'g ©d O) 5 x: O) 81 O) uj

•HC 5 O x: CO

O C O •H 4J m o a; o

a o: r

3—

x * Z \s k OK

//v N

5j,5c.x DT-1087 X,

5 km S DT-1084 (Se)

Figure 48: Reconnaissance geology and sample locations in the area of geochemical anomaly SSM-1. j J

The granodiorite and granite are medium-grained, leucocratic t, o mesocratic, with up to 15 % biotite, White feldspars display incipient fracturing and the rock is similar in composition to the 'granitic gneiss' except that the rock has not undergone crushing and hematization. Northwest to north-northwest trending diabase dikes intrude the plutonic rocks of the area. At one location along a bush road the dike-country rock contact is sheared to a chlorite schist, and is occuppied by a milky-white quarts vein about a metre wide. No sulfide mineralization was observed in outcrop, however, shearing at dike-country rock contacts followed by quarts: flooding is typical in many diabase-associated mineral occurrences throughout the region. The r g f 'an od i or i fees and granites of the area are commonly intruded by white feldspar-quartz pegmatite veins -and dikes which contain visible magnetite and specular hematite. Notably, the area defined by the above average uranium in lake sediment contour also has slightly above average magnetic susceptibi] ity. The coincidence of magnetic susceptibility and higfc} uranium values may be reflecting the above average magnetite and uranium content in the felsic igneous rocks of the area. Although airborne radiometric surveys were not carried out over the area, the (geochemical contours for uranium display some continuity with the [radiometric contours from the Ranger Lake area. These observation's suggest that the lake sediment and water geochemical anomalies in t.herarea are due tp a high uranium content in tht* underlying felsic plutonic rocks, and may also be reflecting the presence of uranium vein-type mineralisation similar to that which occurs in the Montreal River area.

Source of Information O. G. S. -G. S. C. Regional Lake Sedimeint and Water Geochemical Reconnaissance Data, j Eastern Shore, Lake Superior, Ontario; O. F. R. 5226. Source of Information

lib FIELD REPORT TARGET: Geochemical Anomaly, SSM-2 ;i AREA; East of Haviland Bay, Stokely Ski area TOWNSHIP: Tupper twp. DATE OF FIELD INVESTIGATION; ^Se^temter li/ September 14, 1084 U.T.M. CO-ORDINATES: 705,300 mE J j;5, 188,750 mN |; DIMENSION, SHAPE AND ORIENTATION OF ANOMALY:

Long Axis: 10 Km , Short Axis: 5 Km : Orientation: E-W trend • s Shape: Oblong Shajfe ; TOPOGRAPHY OVER ANOMALY: high relief SAMPLES COLLECTED: DT-1092a: Quartz vein A, S DT-1092b: She^r Zone Au - 15 ppb, Cu - 1040 ppm DT-1092c: Granite p DT-1092d: Granite porphyry WR+Tr DT~1093a: Mafic Volcanic A, S DT-1093b: Shear Zone with : sulphides Au s' DT-1094: Diorite , DT-1095: Quarts vein ; s DT-1096: Diabase " DT-1097: Syenodiorite WR+Tr DT-1098: Gabbro-Diabase ' r ^ DT-1099: Granite vein DT-1100: Gabbro ' DT-1101: Metagreywacjce ; DT-1102: Metagrseywacke DT-1103: Amphibolite i WR+Tr DT-1104: Diorite DT-1105: Syenite DT-1 106: Syenodiorite DT-1107: Argillite,; 31ate DT-1108: Greywacke ., pT- 1 109: Diorite ..M lij'-lllO: Granodiorite '" ' - ' i rXT-1111: Diabase ' i : DT-1112: Hornblende Syenite , A - Assay: Au,Ag,etc. S x'jf |ju ^ l i t at i ve Spectronnatric Analysis WR r- Whfj'lft' Rock Chemical Analysis : Tr - Trace Element Analysis i

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t.Q) \ 3 C3* •H TABLE 3: CORRELATION COEFFICIENTS (based on data from O. G. S.-G.'S. C.",- 1979) Geochemical Anomaly SSM-2 Zn vs Mn : .502 Mo vs Mn : , 707 Fe vs Mn : .671 Co vs Mn : .665 Cu vs LOI: .529 Geochemical Anomaly SSM-1 U (S) vs LOI: -.032 U (w) vs LOI: -.28 U (s) vs U (w): .669 Zn vs Fe: '. 626 ; Cu vs LOI: .558 Ni vs Fe: .643 Co vs Mn: .891 Co vs Fe: .935 Mn vs Fe: .68 As vs Mn: .652 Ni vs Fe: ;W43 Co vs Mn: .891 Co vs Fe: .935 Mn vs Fe: .88 As vs Mn: .652 GENERAL GEOLOGY Geological compilation map 2419 (Giblin et al., 1974--76) indicates that the area is underlain by unsubdivided raetavolcanics and metasediments, granites, and outliers of riuronian Supergroup in the area of the geochemical anomaly. Reconnaissance geology in the area indicates the presence of a variety of plutonic rock types consisting of gabbro, diorite, granodiorite, syenodiorite, as well as remnants of Archean metavolcanics and metasediments, Keweenawan volcanics, and argillites and quartsites of the Huronian Supergroup. The plutonic rocks vary in composition from diorite/gabbro to granodiorite, syenite and syenodiorite, becoming felsic towards the east-northeast. Diorite is massive medium-to coarse-grained and equigranular with the feldspars extensively epidotised in some areas. Syenite and syenodiorite are leucocratic, medium-to coarse-grained to pegmatitic, equigranular, and contain chloritised amphibole. Granodiorite to dioritic rocks are generally medium-grained, mesocratic, with an inhomogeneous texture. Amphibolite (metavolcanic) is fine-grained, green to black, and highly magnetic with magnetite grains disseminated throughout the rock. Metagreywacke (amphibolite) is grey-green, consisting of fine-grained layers. A well-exposed fault zone containing sulphide mineralisation (S-4, mostly chalcopyrite and minor sphalerite) occurs in a rock- cut on Highway 17 north of Havilland Bay in mafic (meta)volcanic rocks. Drainage from such rocks and their associated mineralisation could give rise to the anomalous metal concentration in the lake sediments.

Source of Information O. G. S. -G. S. C. 1979: Regional Lake Sediment and Water Geochemical Reconnaissance Data, Eastern Shore, Lake Superior, Ontario; O.F.R. 5226.

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