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Government of Ontario Printed in Ontario, Canada

ONTARIO GEOLOGICAL SURVEY Open File Report 5599

Geology of the Hearst-Kapuskasing Area

by 5.R. Berger 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:

Berger, B.R. 1986: Geology of the Hearst-Kapuskasing Area, District of Cochrane; Ontario Geological Survey, Open File Report 5599, 88p., 6 figures, 11 photos, 3 tables, and 8 maps in back pocket.

Ministry of 2±Fontilnt Northern Development Qi0igt Touflh and Mines Ontario

Ontario Geological Survey OPEN FILE REPORT

Open File Reports are made available to the public subject to the following conditions:

This report is unedited. Discrepancies may occur for which the Ontario Geological Survey does not assume liability. Recommendations and statements of opinions expressed are those of the author or authors and are not to be construed as statements of govern ment policy. This Open File Report is available for viewing at the following locations: (1) Mines Library Ministry of Northern Development and Mines 8th floor, 77 Grenville Street Toronto, Ontario M5S 1B3 (2) The office of the Regional or Resident Geologist in whose district the area covered by this report is located. Copies of this report may be obtained at the user©s expense from a commercial printing house. For the address and instructions to order, contact the appropriate Regional or Resident Geologist©s office(s) or the Mines Library. Microfiche copies (42x reduction) of this report are available for $2.00 each plus provincial sales tax at the Mines Library or the Public Information Centre, Ministry of Natural Resources, W-1640, 99 Wellesley Street West, Toronto. Handwritten notes and sketches may be made from this report. Check with the Mines Library or Regional/Resident Geologist©s office whether there is a copy of this report that may be borrowed. A copy of this report is available for Inter-Library Loan.

This report is available for viewing at the following Regional or Resident Geologists© offices: 60 Wilson Ave. 4 Government Rd. East Timmins, Ont. Kirkland Lake, Ont. P4N 2S7 P2N 1A2

The right to reproduce this report is reserved by the Ontario Ministry of Northern Development and Mines. Permission for other reproductions must be obtained in writing from the Director, Ontario Geological Survey.

V.G. Milne, Director Ontario Geological Survey

iii

FOREWORD

HEARST-KAPUSKASING AREA Semi-detailed geological mapping of the Hearst-Kapuskasing area was undertaken by the Ontario Geological Survey, Ministry of Northern Development and Mines as part of the Special Projects Assisting Resource Communities or SPARC program. The Hearst-Kapuskasing area was selected for mapping on the basis of absence of previous detailed geological mapping and to identify the economic potential of this area that stroddles this portion of the Quetico-Wawa Subprovinces boundary.

V. G. Milne Director Ontario Geological Survey

v

ABSTRACT

The Hearst-Kapuskasing area covers 1075 km 2 between Latitudes 49 0 07©05" and 49 0 19©05" and Longitudes 82 0 52©30" and 83*45© west. The towns of Hearst and Kapuskasing are each about 60 km north of the central part of the map area. Supracrustal rocks composed of mafic, intermediate and felsic metavolcanics, their intrusive euqivalents, and metasediments underlie the central and northern parts of the map area and lie within the Quetico Subprovince. Gneissic rocks composed of progressively metamorphosed and deformed supracrustals were intruded by felsic plutonic domes in the southern and eastern parts of the map area and are within the Wawa Subprovince. The contact between the gneisses and the supracrustal rocks is considered as the boundary between the two subprovinces. At least two periods of deformation have affected the map area with the older, D-j deformation characterized by east-trending fold axes and lineations and the younger, D2 deformation characterized by northeast-trending fold axes and lineations. The supracrustals were regionally metamorphosed from middle to upper greenschist facies under temperature and pressure conditions estimated to be 500-525 0 C at 4 to 5 kbar. Contact metamorphic aureoles developed in metasediments adjacent to granitic pegmatite plutons attained amphibolite grade conditions with temperatures estimated between 550-700 0 C at 4 to 5 kbar. Sillimanite and quartz aggregates preserved

vi i in the granitic pegmatites indicates minimum melting temperatures of 725 0 C at 5 or more kbar. Five geological environments that could host economic mineralization were recognized. Gold and base metals may occur in felsic metavolcanics throughout the area, in association with faults or folds, in association with intermediate pyroclastics and debris flows and in association with the numerous ironstone occurrences. Pegmatites in the west and southwest are potential hosts for molybdenum, tin and rare element deposits.

IX

CONTENTS Abstract i ...... vii Introduction ...... l Location and Access...... l

Topography and Drainage ...... 3 Previous Work i...... 3 Present Geologicai Survey ...... 4

Acknowledgements ...... 5 General Geology ...... 6 Table of Lithologic Units ...... 78

Late Archean ...... 8 Metavolcanics...... 8

Mafic and Intermediate Metavolcanics...... 8 Petrographic Summary ...... 11 Felsic Metavolcanics ...... 12 Petrographic Summary ...... 15 Metasediments ...... 16 Petrographic Summary ...... 18 Mafic and Intermediate Intrusions...... 20 Petrographic Summary ...... 23 Migmatites-Gneiss ...... 23 Petrographic Summary ...... 25 Felsic Intrusions ...... 27 Stray Lake Pluton ...... 27 Felsic Plutons Intruding Gneiss ...... 27 Granitic Pegmatite ...... 29 Proterozoic and Archean Mafic Intrusions ...... 32

Diabase ...... 32

xi

Cenozoic ...... 33 Quaternary...... 33 Pleistocene and Recent ...... 33 Petrochemistry ...... 34 QAP Diagram ...... 34 CaO-Na2 0 © K 2 0 Diagram ...... 37 AFM Diagram ...... 37 Si02 vs NagO K2 0 Diagram ...... 38 3ensen Cation Plot...... 38 Structural Geology...... 40 Summary ...... 40 First Deformation(Di)...... 40 Second Deformation (02)********-**-*--*---**-*----***-**41 Metamorphism ...... 43 Economic Geology ...... 47 Description of Properties...... 48 Robert Campbell Property...... 48 Kenogamisis Gold Mines Limited...... 48 Macassa Mines Limited...... 49 Steve Vukmirovich...... 50 Mike Wabano...... 50 Recommendations for Future Exploration...... 51 References...... 56 Figures...... 64 Photos...... 70 Tables...... 78

xi 11

LIST OF PHOTOS

Photo 1: Pillowed Basalt 70

2: Intermediate Pyroclastic Breccia 70

3: Felsic Pyroclastics 71

4: Quartz-Muscovite Schist 72

5: Bedded Wackes 73

6: Folded Ironstone 73

7: Sillimanite Aggregates in Pegmatite 74

8: Tourmaline in Pegmatite 75

9: DI Fold and Lineation 76

10: D2 Interference Fold Pattern 76

11: Bedding Transposed by Second Deformation 77 LIST OF FIGURES

Figure 1: Location Map 64 2: QAP Diagram 65 3: CaO-Na20-K2 0 Diagram 66 4: AFM Diagram 67 5: Si02 vs NaaO K2 0 Diagram 68 6: Jensen Cation Plot 69 LIST OF TABLES Table 1: Table of Lithologic Units 78 2: Selected Whole Rock Analyses 79 3: Assay Results 82

XV

Geology of the Hearst-Kapuskasing Area District of Cochrane by Ben R. Berger

xvi i

-1- Introduction The Hearst-Kapuskasing area was mapped to better define a supracrustal sequence previously mapped at 1 inch to 2 miles during Operation Kapuskasing (Bennett et al. 1967). To this end, semi-detailed mapping at 1:15,840 (1 inch to 1/4 mile) scale was carried out to identify the major supracrustal lithologies, economic mineral occurrences and environments for potential economic mineralization. This project was part of the Special Projects Assisting Resource Communities or SPARC program and was made possible through in-year supplementary funding by the Government of Ontario. Location and Access The Hearst-Kapuskasing area covers 1075 km2 (387 m^ ) between Latitudes 49O07©05" N and 49O19©05"N, and Longitudes 82O52©30"W and 830^5©w (Fig. 1). The map area covers all of Caithness, Rykert, Fergus and Ecclestone Townships, and part of Scholfield, Pelletier, Doherty, Abbott, Opasatika and Bourinot Townships. The towns of Hearst and Kapuskasing, major supply points on t Highway 11, are both 60 km north of the central part of the map area. From Hearst the western third of the area can be accessed via Highway 682 south to the all-weather gravel Caithness Forest Access Road. Numerous private logging roads constructed by Oomtar Incorporated service most of Pelletier, Doherty, Caithness -2- and Scholfield Townships. These roads are in various stages of repair and generally can be used only during dry weather, snow- less conditions. Several bridges spanning the Mattawitchewan River were washed out during 1985 stopping truck access to most of Caithness Township. Three and four wheeled ATC©s were used to map this area. New logging roads are continually being built, especially in Doherty Township, which will continue to improve access and expose new bedrock outcrops. The Goat and Mattawitchewan Rivers are navigable during periods of high water and provide access to parts of Pelletier, Scholfield and Caithness Townships. These rivers have eroded the overburden to bedrock, consequently outcrop is more plentiful than elsewhere in the area. From Kapuskasing the eastern two-thirds of the area is accessible by the Cargill-Bourinot Forest Access Road or by Highway 11 to the Fergus road. Major internal access routes include the Ecclestone and Abbott forest access roads which are maintained by Spruce Falls Power, Pulp and Paper Company Limited. Several logging roads off of the access routes cover most of the area. Although logging operations are still progressing the main activity occurred in the 1970©s so that many of the secondary roads are unused and vegetation infringes along the road sides. At the time of writing roads maintained by Spruce Falls Power, Pulp and Paper Company Limited did not connect with Domtar Incorporated roads, effectively dividing the -3- map area into two segments. The Missinaibi River is a major waterway providing north- south access across the central part of the map area. It is a well travelled canoe route with cut and marked portages around its many rapids. The Opasatika River in the eastern part of the area is navigable during high water and provides access to the area north of Rufus Lake. Topography and Drainage The topography of the area is flat with average relief between 3 to 5 m and maximum relief of 30 m in Doherty Township. Lacustrine clay and till cover large parts of the area and out crop is poorly exposed especially in the north. All lakes, creeks and rivers eventually flow into the Missinaibi River which is part of Hudson Bay-Games Bay water shed. Rufus Lake, the largest in the map area, is part of the headwater for the Opasatika river. The flat topography prohibits development of good drainage resulting in extensive swamps, tag alder and small ponds. Bedrock structures locally control drainage patterns but Pleistocene features exert a more general regional control. Previous Work In 1875 Robert Bell, returning from James Bay to Lake Superior, mapped along the Missinaibi River (Bell 1877). In 1903-05 W.3. Wilson and W.H. Collins mapped along the Missinaibi River and around Big Pike Lake as part of a regional mapping program. More recently Bennett et al. mapped the area in 1966 as part of the helicopter supported ©Operation Kapuskasing© (Bennett -4- et al. 1967). This program produced 1 inch to 2 mile preliminary maps generalized to produce the 1 inch to 4 mile geological compilation series map 2166, the Hearst-Kapuskasing sheet. Until the present project, Operation Kapuskasing provided the most detailed coverage of the map area. Several people (Thurston et al. 1977, Watson, 1980, Card et al. 1980, 1981, Card 1982, Sage 1983a, Percival 1985) have worked in adjacent areas and their results either directly or implicitly relate to the present project. Readers should consult the reference list of this report for complete bibliographies. Present Geological Survey Field work summarized in this report was carried out in the summer of 1985 by a seven person crew consisting of one geologist, two senior assistants and four Junior assistants. Mapping was done at 1 inch to 1/4 mile (1:15,840) scale using 1 inch to 1/4 mile airphotographs supplied by Silviculture Section, Public Service Centre, Ministry of Natural Resources. Outcrop areas were plotted in the field on acetate overlays to the airphotographs; the data were transferred to cronoflex base maps prepared by the Cartography Section, Surveys and Mapping Branch, Ministry of Natural Resources, from Forest Resources Inventory Maps (scale 1 inch to 1/4 mile or 1 to 15,840) of the Timber Branch of the Ministry of Natural Resources. Given the large map area, readily accessible outcrops were given priority. In practice this meant outcrop along or near roads and rivers were mapped in preference to isolated outcrop areas. Traverses into isolated critical areas or those areas -5- supposedly underlain by metavolcanics were carried out as time permitted. Helicopter support was used for a three day period to map isolated areas, and map otherwise inaccessible outcrops. Although every effort was made to examine as much outcrop as possible there were several outcrops not mapped during the present survey. Acknowledgements P.L. Roy and D.W. MacMillan in their capacity as senior assistants conducted independent mapping and were responsible for mapping over 50 percent of the area. B.E. Chapman, G.D. Sherrer, V.L. Wasiuta and M.W. Hitch were Junior assistants and Wasiuta and Hitch carried out a few independent traverses. P.L. Roy capably served as winter assistant on this project and is responsible for much of the thin section examinations, modal analyses of rocks, staining and point counting of rock slabs and some of the drafting. Ministry of Natural Resources personnel in Hearst and Kapuskasing provided support throughout the summer. In particular, use of the Goat River silviculture camp by the Hearst MNR staff is gratefully appreciated. D. Goodwin of the Kapuskasing MNR provided valuable information and assistance which is gratefully acknowledged. Spruce Falls Power, Pulp and Paper Company Limited and Domtar Incorporated personnel provided logging road locations and access without which the mapping could not have been completed. The skills of pilot G. Stubbs and engineer C. Waugh of Ranger Helicopter of Sudbury are greatly appreciated and their -6- expertise made the helicopter mapping simple. GENERAL GEOLOGY The map area is underlain by rocks of Precambrian age of the Superior Province of the Canadian Shield. Supracrustal rocks composed of metavolcanics, their intrusive equivalents and meta- sediments underlie the central and northern parts of the area and gneissic rocks intruded by domal felsic plutons underlie the southern and eastern parts of the area. Based on general descriptions and previous work by McGlynn (1970), Thurston et al. (1977), Card et al. (1980, 1981) Card (1982) and Percival and Card (1985) the supracrustal rocks are part of the Quetico Sub- province and the domal gneiss terrain is part of the Wawa Sub- province. It would appear that the contact between the supra crustal rocks and the gneissic terrane represents the division between the two subprovinces. This contact where not intruded by granitic pegmatite is characterized by a rapid metamorphic progression from supracrustals to para- and orthogneiss. At least two periods of deformation have affected the supra crustal rocks and brittle deformation related to the latest event is responsible for development of the Rufus Lake Fault in the east part of the area. Amphibolite rank contact metamorphic aureoles developed in supracrustal rocks adjacent to granitic pegmatite plutons are locally superimposed upon regional middle to upper greenschist rank metamorphism. Note that in the following descriptions of supracrustal units all rocks have been metamorphosed, none have retained their original mineralogy and/or texture. The prefix "meta" has -7- been omitted for brevity when referring to individual rock types and will only be used in the general sense i.e. metasediments and metavolcanics.

Migmatitic rocks underlie a significant portion of the map area. "Orthogneiss", "paragneiss", "metatexite", and "diatexite" are terms used to subdivide the migmatites and are specific for the map area. Ortho- and paragneiss are used to describe rocks with recognizable igneous and sedimentary protoliths respectively (AGI 1980). They retain a strong planar fabric subparallel the regional foliation and gneissosity is poorly developed. Metatexite is a rock produced by metamorphic differation and partial fusion in which migmatitic banding is evident (Brown, 1973). In the map area the paleosome (parent rock) is of unrecognizable origin and the neosome (new rock) occurs in variable quantities (from 10 to 80 percent of the rock). Gneissosity in metatexites is subparallel the regional structural trends although perturbations are common. Diatexite is a rock formed by high-grade anatexis in which fusion may be complete and in which there is no continuous migmatitic banding (Brown, 1973). Further, in the map area, schlieren and other "turbulent" structures are characteristic of inhomogeneous diatexite (Mehnert, 1968). Structural trends, if present are discordant with regional foliation. Table 1 summarizes the rock types in the map area. -8-

LATE ARCHEAN METAVOLCANICS MAFIC AND INTERMEDIATE METAVOLCANICS The mafic and intermediate metavolcanics are recognizable in the field by their green to dark green weathered surfaces which reflect the predominance of hornblende as the major mafic constituent. The most common rock type is massive to foliated amphibolitic flows that occasionally contain amygdules but are generally devoid of primary structures. Where primary structures such as pillows, pillow breccias and tephra are recognized they have been mapped but their degree of preservation varies greatly throughout the map area. A separate unit composed of quartz, feldspar and epidote knots and stringers in a dark green highly deformed matrix occurs in the western part of the map area. These quartz, feldspar and epidote concentrations were also observed in the centres of many pillows and are interpreted to be the alteration products of coalesced varioles. The unit composed of knots and stringers may represent highly deformed, pillowed flows. Pillows are common features in the rocks in the western part of the map area. Average pillow sizes are 50 cm (photo 1) and maximum sizes up to 2 m in long axis are present. Pillowed flows are generally close packed with dark green to black resistant selvages averaging 1 to 3 cm thick. Stratigraphic top indications are rare compared to the volume of flows due in large part to deformation. Pillows with delicate concentric cooling cracks ("onion skin") are preserved at the Junction of the Synco -9-

Road with the Caithness Forest Access Road in Pelletier Township. Pillow breccias are minor components of the mafic and intermediate metavolcanics. They form narrow, discontinuous units where they are interlayered with flows; however, they are more continuous where they are interbedded with greywackes and interflow metasediments in Scholfield Township. Pillow breccias are difficult to recognize as the weathered surface is similar to mafic flows or amphibolitic metasediments. Careful examination is required to determine fragment outlines. Mafic and intermediate pyroclastic rocks occur predominantly in the eastern part of the map area although some units are present in the western part. The coarser lapilli tuff and pyroclastic breccia units contain white weathering intermediate to felsic clasts in a green to brown matrix (Photo 2a). Close examination of these units usually reveals that highly stretched mafic clasts are also present (Photo 2b). Tuff and some lapilli tuff units contain only mafic clasts and are easily confused in the field with massive or foliated flows. Generally, the development of close-spaced foliation planes and a fissile habit distinguishes a tuff from a flow. Debris flows were mapped in west-central Ecclestone Township. These units are heterolithic containing rounded and angular, amygdaloidal, basaltic scoria, angular to rounded chert fragments occasionally retaining laminations and a minor quantity of sulphide fragments. The clasts are unsorted, supported in a mafic tuff matrix and are generally chaotically organized. Poor exposure prevents vertical and lateral correlation with other -10- units; however, intermediate pyroclastics are nearby. The poor sorting, matrix-supported clasts and chaotic organization are characteristic of debris flows in a subaqueous or subaerial environment (Williams and McBirney, 1979, Macdonald, 1972). In the map area there is no definitive evidence for subaerial environments but plenty of evidence (pillowed flows, turbidites) for a subaqueous one. The debris flows likely formed subaqueous- ly by avalanching material from the flanks of a volcanic edifice and these avalanches had enough power to rip up previously consolidated chert and sulphide ironstone beds. Massive to foliated amphibolitic flows generally devoid of recognizable primary structures comprise the bulk of the mafic and intermediate metavolcanics. These rocks are fine to medium grained, recrystallized, and weakly to strongly foliated. Hornblende is the dominant mineral and commonly comprises 50 to 65 percent of the rock. In Caithness Township intermediate flows comprise a distinctive subunit. These rocks have a colour index of 25 to 30, are massive and light brown to buff weathering. In thin section they contain quartz, plagioclase, and hornblende and appear to be the extrusive equivalents of a hornblende monzonite intrusion in Pelletier Township (see Mafic to Intermediate Intrusions, page 20). The mafic to intermediate metavolcanics underlie the central portion of the map area. A linear belt varying from 1 km to 5.7 km wide extends from the western boundary to Rykert Township in the center of the map area. Pillow tops face predominantly south -11- but local reversals In younging direction indicate folding has occurred. Overturning of the strata is prevalent along the southern contact of the metavolcanics with the overlying meta- sediments and felsic metavolcanics. Intermediate pyroclastics interlayered with mafic flows and tuffs underlie parts of Opasatika, Fergus and Ecclestone Townships. Younging direction is unknown and structural trends indicate complex folding of the strata has occurred. Although there is a gap between the western and eastern segments, pyroclastic breccias in Ecclestone Township are similar in composition and morphology to pyroclastic breccias observed in Rykert Township. Basaltic sills and dikes are found intruding metasediments along the Mattawitchewan River in Caithness Township. Both sills and dikes are narrow (50 cm to 100 cm) black weathering, fine grained, aphanitic rocks. The metasediments are waterworn by the Mattawitchewan River and consequently the dikes and sills stand in relief and are easily identified. They are likely more abundant than indicated by mapping. Petrographic Summary of the Mafic and Intermediate Metavolcanics All mafic to intermediate metavolcanic rocks examined in the t map area have the mineral assemblage: 1) hornblende * plagioclase (An35,gQ) -t- quartz * epidote * chlorite * garnet * biotite. Sphene, magnetite and sulphides are common accessory minerals. Calcite is commonly developed in the eastern but is absent in the western part of the area. Garnet visible in hand specimen is -12- frequently developed in the matrices of the pyroclastic units but occurs microscopically in flows as well. Sericite and muscovite are present in alteration veinlets and rarely as byproducts of plagioclase degradation. Quartz often shows overgrowths and plagioclase is often compositionally zoned. Chlorite occurs around the edges and along cleavage planes of biotite and/or hornblende crystals. It appears to have destroyed the host mineral and for this reason is considered to be retrograde in origin. In most thin sections blue-green pleochroic hornblende displays a weak to strongly developed crystallographic orientation which is expressed as a lineation where measurable in hand samples. Hornblende occurs as well formed blades, large polkiloblasts or as well formed basal sections showing two cleavages. Plagioclase and quartz usually occur between hornblende crystals. Felsic Metavolcanics Felsic metavolcanics are composed of dacite to rhyolite flows, pyroclastics and subvolcanic intrusions (see Petro chemistry, page 3*f). The flows weather white to pale yellow, contain abundant quartz "eyes" up to 2 mm in diameter and are common in the western part of the map area. These rocks are fine grained, aphanitic units containing quartz, epidote and sericite. At the Junction of two logging roads in northwest Doherty Township a felsic flow (10 m thick) less between underlying pillowed basalts and overlying pyritic, amphibolitic metasediments. Felsic flows such as this comprise the tops of -13-

minor "volcanic cycles" and are common in the map area. Poor exposure, however prevents correlation of these units thus inhibiting the development of a regional stratigraphy. Pyroclastic breccias, tuffs and minor flows form a felsic unit discontinuously exposed for 13 km along strike in Pelletier and Doherty Townships. Tuff and pyroclastic breccias (clasts up to 25 cm) and lapilli stones (average clast size 6 to 7 cm) are mostly heterolithic with essential dacite and rhyolite clasts predominant over mafic and accidental sulphide fragments. The clasts are close packed and the small amount of matrix that is present is composed of felsic ash to small lapilli (1 mm to 10 mm). Most commonly the matrix was deformed to a quartz-sericite schist. The tuffs contain ash to small lapilli in a quartz-rich matrix and are commonly bedded. These tuffs are volumetrically subordinate to the breccia deposits and occur interbedded with coarser units and along their northern contact with clastic metasediments. Partial assimilation by granitic pegmatite, and deformation

L obscure stratigraphic and contact relationships of the pyroclastics. Where this occurs, relict clasts and quartz "eyes" are diagnostic features that serve to distinguish these units (Photos 3a, 3b). Felsic subvolcanic intrusive rocks occur as feldspar porphyry dikes throughout the map area and quartz-feldspar porphyry to granodiorite intrusions spatially restricted to the Rufus Lake Flatt Lake area. The feldspar porphyries are light grey to brown weathering dikes 1 to 3 m thick with feldspar phenocrysts variable from microscopic to 2 to 5 mm size. They normally crosscut the stratigraphy but may be subconcordant in places. The subvolcanic pluton northwest of Rufus Lake is composed of predominant quartz-feldspar porphyry and subordinate grano diorite and feldspar porphyry. Related dikes of similar composition intrude the host mafic metavolcanics. The intrusive rocks weather white, pink and brown depending on the rock type and vary from porphyritic to equigranular. Cataclastic to mylonitic textures overprint original textures near the Rufus Lake fault where an important subunit of the pluton is now quartz-muscovite schist (photo 4). The schist is most extensively developed near the Rufus Lake fault where basalt and sulphide facies ironstones are tectonical- ly interleaved with the schist. Pink weathering granodiorite intruded by pyrite- and epidote-bearing quartz veins is a minor component in this area. The quartz-muscovite schist which is commonly crenulated is not as abundant west of the fault and in this area quartz- feldspar porphyry is the protolith. The quartz-feldspar porphyry is white weathering and contains quartz and feldspar phenocrysts. The rock is medium grained to porphyritic and inperceptibly grades into both feldspar porphyry and granodiorite. In northern Fergus Township a few outcrops of rhyolite flows are exposed (see Petrochemistry page 34). These rocks are hornblende and feldspar phyric with a grey aphanitic groundmass. -15-

They are generally massive to llneated and are Interlayered with clastic metasediments. Poor exposure prohibits delineation of the unit and possibly more felsic metavolcanics underlie this area. Petrographic Summary of the Felsic Metavolcanics Felsic metavolcanics are characterized by the mineral assemblage:

1) quartz * plagioclase -f muscovite * chlorite * epidote i brown biotite garnet. Apatite, hornblende, actinolite, microcline and orthoclase are common accessory minerals. Chlorite is commonly retrograde after biotite but in at least one thin section chlorite appears to have prograded to biotite. Phyllosilicates commonly form with a preferred orientation that defines the foliation in the rocks. Original ash and lapilli are recrystallized and difficult to distinguish in thin section. Garnet is usually microscopically present as clear anhedral to euhedral crystals. The felsic subvolcanic rocks are characterized by the mineral assemblage:

2) quartz * plagioclase * epidote * muscovite * chlorite green or brown biotite microcline. Sphene, apatite, hornblende and garnet are common while zircon, allanite and calcite are rare. Compositionally zoned euhedral feldspar phenocrysts and porphyritic textures distinguish the subvolcanic pluton from other felsic plutons in the map area. Chlorite is retrograde after biotite and is predominantly iron-rich. Preferred orientation of phyllosilicates and quartz -16- gralns is well developed in mylonitic rocks and poorly developed in less tectonized rocks. Garnets are anhedral to euhedral, clear, microscopic crystals. METASEDIMENTS Metasediments are the most abundant lithology in the map area. Clastic metasediments predominate and are subdivided into wackes, amphibolitic metasediments and volcanogenic wackes or reworked tuffs. Volcanogenic wackes are light brown to dark grey weathering and contain up to 5056 volcanic detritus (ash) in a quartzo- feldspathic matrix which distinguishes them from normal wackes. They are generally thickly bedded and show no internal organization although they are occasionally thinly bedded near contacts with the felsic metavolcanics. Volcanogenic wackes are dispersed throughout the metasediments but tend to concentrate near metavolcanic contacts. Amphibolitic metasediments weather dark green to black and contain over 50 percent hornblende. Magnetite and garnet are common accessory minerals and quartz is minor or absent. Beds are thick (50 cm) and massive to laminated with no internal organization. Amphibolitic metasediments occur as interflow units, interbeds between wackes, and as beds laterally or vertically associated with ironstones. Wackes comprise the dominant unit of the clastic meta sediments (Photo 5). They weather light brown to grey and have two major modes of occurrence. Wackes are well bedded and display grain size variation or -17- occur as wacke-pelite couplets which are turbiditic in origin. In the second mode of occurrence wackes are thin to thickly bedded, display no internal organization and contain abundant biotite or hornblende. The wackes display little lateral or vertical variation throughout the map area. Detrital grains, although recrystal- lized, are inferred to have been sand-sized or smaller. There is very little evidence for high energy environments as conglomerates are absent and "rip-up" clasts are rare. The clastic metasediments are compatible with a distal, moderate to low energy environment (Walker, 1979). Chemical metasediments are represented by chert and sulphide-oxide facies ironstones. Chert usually occurs in association with ironstones, however, occasionally it occurs as isolated beds in wackes or associated with pillow breccia and mafic tuffs. These isolated beds are white weathering, thinnly bedded to laminated and recrystallized to fine grained sugary quartz. They are not to be confused with quartz veins which are composed of clear to milky quartz and are discordant to bedding. Chert in association with ironstone occurs as 2 to 30 cm thick layers interbedded with mixed hornblende, magnetite, quartz, sulphide and garnet-bearing beds of equal thickness. These cherts are extensively recrystallized but occasionally retain laminations. Ironstones occur in close spatial association with mafic to intermediate metavolcanics and in many cases occur at the contact between metavolcanics and clastic metasediments. -18-

Ironstones interbedded with mafic flows contain up to 10 percent sulphides and magnetite in a dark green to black hornblende-rich matrix. These units are narrow, 1 to 3 m thick and continuous unless transposed by deformation. They are easily identified in the field by their gossany weathered surfaces. Ironstones interbedded with clastic metasediments or near metavolcanic-metasediment contacts contain 5 to 90 percent mixed sulphides and magnetite. Pyrite and pyrrhotite are the major sulphides with graphite and trace chalcopyrite as accessory minerals. The ironstones vary from 1 to 10 m in thickness, but in Pelletier Township south of the hornblende monzonite intrusion, ironstone and mafic tuffs occur in a fold thickened sequence up to 250 m thick (Photo 6). Iron staining and gossan development are usual components of these ironstones. The close spatial association with metavolcanics suggests an exhalative origin for the ironstones. As such the ironstones represent favourable environments for metallic ore deposits. Petrographic Summary of the Metasediments The metasediments are divisible into the following major metamorphic assemblages which reflect original composition. These assemblages are: in wackes and semipelites; 1) quartz * plagioclase * biotite * garnet ± chlorite * muscovite * epidote cordierite: at higher metamorphic grade the assemblage becomes: 1a) quartz * plagioclase * biotite -t- garnet -i- sillimanite * -19-

muscovite t cordierite * microcline * staurolite, in pelites 2) quartz -t- plagioclase * hornblende t garnet * biotite * chlorite * epidote cordierite: at higher metamorphic grade the assemblage becomes: 2a) quartz * plagioclase * hornblende -f cummingtonite * garnet * biotite * chlorite * cordierite. in ironstones: 3) Hornblende * quartz * epidote * magnetite * sulphide * garnet * chlorite * plagioclase biotite: no higher grade assemblage was observed. The first and most common, mineral assemblage was developed in wackes specifically semi-pelites and/or aluminous beds. The second mineral assemblage developed in the more mafic pelite beds and the third assemblage in the ironstone units. The meta- sediments have undergone polyphase metamorphism and deformation resulting in poor preservation of primary textures and structures. The resultant fabric is predominantly metamorphic and several mineralogical relationships are apparent either in the field or in thin section. The metasediments have an anisotropic fabric with phyllosil- licates and amphiboles showing a strong preferred orientation in most thin sections. In many samples the phyllosilicates over print a previous foliation. With a few exceptions, chlorite occurs as a minor constituent in retrograde relationships often with biotite and/or hornblende. Garnet, visible in hand sample, is helicitic in thin section and commonly post-kinematic. Garnet -20- more commonly occurs as clear, euhedral microscopic crystals In virtually all thin sections examined. Both habits of garnet can occur together. With respect to metamorphic grade mineral assemblages 1, 2 and 3 are compatible with middle to upper greenschist facies, mineral assemblages 1a and 2a are compatible with amphibolite facies (Winkler 1967). For a more detailed description refer to the "Metamorphism" section of this report. In the field metasediments at amphibolite facies develop distinctive sillimanite, muscovite and/or microcline porphyrob- lasts. The porphyroblasts vary from 2 to 15 mm and are restrict ed to metasediments in the proximity of granitic pegmatite plutons in the west and southwest parts of the map area. Tourmaline is the most significant accessory mineral. It is restricted to metasediments in the south and southwest parts of the area. Its presence indicates boron was introduced into the rocks either originally as detrital tourmaline or by later meta somatism. MAFIC AND INTERMEDIATE INTRUSIONS Mafic and intermediate intrusions vary in composition from biotite-pyroxene gabbro to monzonite. Biotite-pyroxene gabbro is a green, knobby textured rock that resembles peridotite in the field. It occurs as dikes intruding gneiss in Abbott Township where it coincides with a prominent aeromagnetic high (ODM-GSC Map 2237G, Opasatika Lake 1963c). Spatially associated with the dikes are magnetite segregations up to 2 cm and asbestiform serpentine along some fractures in the dikes. Biotite-pyroxene -21- gabbro also occurs in Pelletier Township near the hornblende monzonite intrusion. In both occurrences the rock appears relatively unaltered and in thin section contains 25 to 30 percent biotite, 20 to 30 percent clinopyroxene, 20 to 40 percent plagioclase (An5Q-7i) and up to 10 percent calcite. In contrast to the previous rock type the field name pyroxenite was applied to soft, grey-green weathering units. These rocks contain relict pyroxene crystals which have largely recrystallized to hornblende, chlorite and minor biotite. Pyroxenites occur as small isolated units within the mafic and intermediate metavolcanics and as large megacrystic xenoliths in the gneiss. In the former occurrence pyroxenites are part of the supracrustal stratigraphy but their lateral and vertical continuity is very limited due mainly to poor exposure. In the second mode of occurrence megacrystic hornblende (up to 2 cm) often with pyroxene cores form an interlocking lattice of crystals preserved as large xenolithic blocks in the gneiss. Gabbro intrusions are recognized in the field by their coarse grained, equigranular massive texture in contrast to the finer grained foliated mafic flows. Hornblende, plagioclase, epidote and talc are the major constituents with minor chlorite, magnetite and garnet. The largest gabbro body is in southwest Rykert Township and occurs as a sill-like intrusion in mafic metavolcanics. The largest intermediate intrusion is a hornblende monzonite pluton in Pelletier Township. The pink to white weathering rocks frequently contain mafic metavolcanic xenoliths, epidote, and red -22- hematite, and potassium veining which increase in number near the contacts. Petrographic examination of a limited suite indicates the pluton ranges from monzogabbro to syenite in composition (Figure 2). Blue green pleochroic hornblende is the major mafic mineral with plagioclase (An^o-69)* microcline and Q-10% quartz. Biotite, epidote and chlorite are common accessories with sphene, apatite and garnet present in trace amounts. Monzonites occur in the Superior Province as phases of larger composite plutons (Percival et al. 1985) and in spatial association with gold deposits in the Abitibi Subprovince (Ayres and Cerny, 1982). In the former setting plutons border supra- crustal-gneiss assemblages and in the latter plutons are late tectonic bodies intruding supracrustal assemblages. Elements of both tectonic settings occur in Pelletier Township. The origin of monzonitic and related granitoid rocks is controversial and numerous theories are presented by Ayres and Cerny (1982) and Hatch et al. (1972). Given the numerous xenoliths and stoping at the contacts of the monzonite in Pelletier Township contamination appears to have been important. A pink weathering pegmatite composed of large (1 cm) plagioclase crystals in a hornblende-magnetite matrix is exposed on the southeast shore of Fergus Lake. A finer grained equivalent is exposed further west. Both occurrences intrude clastic metasediments. Feldspar staining of the pegmatite revealed less than 15 percent potassium feldspar was present indicating the rock is mafic to intermediate in composition. These rocks are very magnetic and this suggests the aeromagnetic -23- high around Fergus Lake and area is caused by a large mafic to intermediate intrusion (ODM-GSC Map 2237 G, Opasatika Lake, 1963c). Petrographic Summary of the Mafic and Intermediate Intrusions Primary mineralogy is poorly preserved in the mafic intrusions and is now represented by the assemblage: hornblende -f green biotite * epidote * plagioclase clino pyroxene * garnet * chlorite talc. Clinopyroxene, either diopside or augite, present in most mafic intrusions, is recognizable in hand sample by its bright green weathering. Biotite occurs as well formed dark green pleochroic crystals and has only locally retrograded to chlorite. Hornblende is the most common mafic mineral and is typically pleochroic from dark green to light green. The intermediate hornblende monzonite intrusion is represented by the mineral assemblage: hornblende * plagioclase * microcline -t- chlorite * epidote * quartz * biotite * garnet. The monzonite is equigranular to glomeroporphyritic and is massive to lineated. Feldspars are largely unaltered and considered primary in origin. Hornblende is pleochroic blue- green and several crystals are cored by actinolite which indicates a metamorphic origin for the hornblende. Biotite often replaces hornblende but can occur separately and is inferred to also be of metamorphic origin. Migmatites-Gneiss The gneissic rocks exhibit a wide range of compositional, -24- structural and textural styles. Ortho- and paragnelsses display structural and textural affinities with their supracrustal protoliths in that they retain the regional foliation and are approximately the same grain size. These gneisses appear to have formed in situ by metasomatic infiltration of granitizing fluids (Mehnert 1968). Supporting evidence is derived from ortho- paragneiss mineralogy which includes metavolcanic and meta- sedimentary mineral assemblages (previously described, this report) with the addition of microcline, epidote and sericite. The last three minerals appear to have formed passively as relict primary structures such as bedding, felsic clasts and primary layering are still identifiable in the gneiss. In the least granitized rocks microcline and sericite occur intergranularly or in thin stringers with minimum alteration of pre-existing mineralogy. As granitization proceeds microcline increases proportionately, sericite and epidote selectively replace plagioclase, and pre-existing phyllosilicates are often pseudomorphed by chlorite. Extreme granitization involves development of blastic K-feldspar, pervasive epidotization, total destruction of plagioclase and marks the passage to metatexite. Metatexites comprise a large portion of the gneisses. The paleosome represents metasediments and metavolcanics but no distinction between the two is possible in the field. Neosome comprises 10 to 80 percent of the rock and occurs as granitic pods and veins injected subconcordantly to the regional foliation and as pervasive or patchy granitized blocks gradational with ortho- and paragneisses. Leocosome is quartzo-feldspathic and -25- aplitic, pegmatitic or equigranular. Melanosome occurs as thin discontinuous biotite-hornblende wisps and streaks within the leucosome or along the paleosome-leucosome boundary. Migmatitic banding of melanosome and leucosome is common in heavily injected outcrops. Overall, metatexites are coarser grained and display a greater heterognelty than ortho-paragneiss assemblages. Diatexites are subordinate rock types in the map area and are restricted to the south and around the perpheries of felsic plutons intruding the gneiss. These rocks are generally heterogeneous displaying highly contorted schlieren and raft structures (Mehnert, 1968) which indicates a higher degree of neosome mobility than in other types of gneiss. The high mobility created structural trends in the diatexites which are discordant with regional foliations. Around the perpheries of felsic plutons diatexites are more homogeneous and appear to be gradational into plutonic rocks. Poor exposure often prevents proper delineation between pluton and diatexite; however, occasionally sharp intrusive contacts are observed. Petrographic Summary of the Gneisses The gneisses are represented by the mineral assemblage: 1) plagioclase (An^ 7 . 68 ) * quartz * epidote * hornblende * biotite chlorite sericite garnet ± microcline. Although mineralogically simple the paragenesis of the gneisses is complex. Ortho-and paragneisses have complex metamorphic and structural histories. Pervasive epidote and sericite alteration has destroyed plagioclase and epidote overgrowths on epidote crystals indicates they were subjected to -26- two periods of metamorphism. Pre-existing phyllosilicates have largely retrograded to blue birefringent chlorite the orientation of which defines a preferred orientation. Garnet occurs as small clear, euhedral crystals and large helicitic garnets are absent. Ortho-and paragneisses often contain ribbon-like quartz grains and mortar structure around epidote which Implies cataclasis has affected these rocks. In many thin sections epidote or sericite stringers cut all minerals and define a late stage alteration event. Metatexites and diatexites are extensively recrystallized and are generally less complex mineralogically than the ortho-and paragneisses. Calcic plagioclase (An50-7l) is * el l formed and displays albite and Carlsbad twinning in an interlocking crystal matrix. Poikiloblastic and idioblastic hornblende and biotite are the major mafic minerals and often define a preferred orientation. Chlorite is less abundant than in the ortho-and paragneisses and is absent in many thin sections. Epidote is widespread throughout the rocks as anhedral crystals and occasional overgrowths indicate that a second period of metamorphism occurred. Garnet is common as clear, euhedral crystals. Large, helicitic garnet is restricted to sericite- epidote veinlets and is uncommon in these gneisses. Calcium and potassium alteration is largely confined to veins although patchy pervasive alteration is present. Zoned veins containing epidote cores and microcline-sericite rims are present but monomineralic veins are more common. Mortar structure, ribboned quartz grains and microscopic ductile shearing indicate cataclasis affected -27- some of the gneiss. At least some of the diatexites crystallized from melts as indicated by myrmekitic and graphic intergrowths. FELSIC INTRUSIONS Stray Lake Pluton The Stray Lake Pluton intrudes metasediments in northern Scholfield, Caithness, and Rykert Townships and extends north of the map area. The pluton is leucocratic with a prominent penetrative foliation defined by alignment of elongated quartz grains, biotite or hornblende crystals. The foliation is generally parallel to the assumed contacts of the pluton and displays moderate to shallow dips. This implies the foliation might be primary and the Stray Lake Pluton may have been emplaced diapirically. The intrusion is composed of equigranular white weathering granodiorite (Figure 2). Biotite and hornblende comprise approximately 10 percent of the rock with biotite much more abundant. Epidote is always present as interstitial grains and as a prograde metamorphic mineral after biotite or hornblende. Plagioclase is commonly altered to sericite although some crystals are relatively fresh. Garnet is a common accessory mineral and in the presence of epidote is considered to be metamorphic in origin. Microcline is the major alkali feldspar and although come crystals appear to be original, some microcline is localized in stringers with sericite and epidote indicating metasomatism has affected some parts of the pluton. Felsic Plutons Intruding Gneiss -28-

Several tonalitic to granitic plutons intruding the gneisses are syn- to post-tectonic. Syn-tectonic components of these plutons are easily confused in the field with the gneisses as they, in part, have gradational contacts with the gneisses and locally preserve gneissic xenoliths. In thin section the syn tectonic rocks are similar to the meta- and diatexites in style of deformation and alteration products. Plagioclase is still predominantly calcic (An5Q-7()) although more sodic plagioclase (An28-*fO) is present. Hornblende and green biotite are the major mafic minerals. In contrast with the gneisses, these plutons are light grey to pink weathering with a poor to well developed foliation, as opposed to gneissosity, defined by the alignment of quartz grains and platey minerals. Mafic minerals comprise less than 25 per cent and commonly less than 15 percent of the rock. A characteristic feature of the plutons is the absence of granitic dikes which are common in the gneisses. The post-tectonic components of these felsic plutons are coarse grained, equigranular and distinct in the field and petro- graphically. In the field, post-tectonic rocks are white weathering and usually massive. Locally, foliation defined by closely spaced fractures as opposed to mineral alignment is present. In thin section minerals are mostly fresh and unstrain ed. Plagioclase is albitic and occasionally is antiperthic with microcline. Allanite, zircon and sphene are ubiquitous. Idio morphic epidote often with worm-like intergrowths of quartz is commonly associated with green pleochroic biotite. -29- Tonalitic, granodiorite and granitic phases of these plutons are inseparable in the fieid because of their common white to grey weathered surfaces and fairly constant quartz content (20 to 30 percent) and constant total feldspar content (45 to 60 percent). A limited suite was stained for feldspars and the results are presented in Figure 2. Quartz monzonite occurs as part of the larger plutons and as separate plutons intruding the gneisses. These rocks are mineralogically and compositionally similar to the monzonite intrusion in Pelletier Township except they contain, on average, 10 to 15 percent quartz. This rock type is not represented on Figure 2. All felsic plutons intruding the gneisses appear to exert local influence on the gneissosities of the host rocks. In several places gneissosities are parallel the assumed contacts of the plutons suggesting the intrusions were emplaced as domes. This feature is characteristic of the gneissic terrain in this part of the Wawa Subprovince (Percival and Card, 1985). GRANITIC PEGMATITE In the west and southwest parts of the map area granitic pegmatite intrudes the gneisses and the supracrustals. The pegmatite is easily recognized in the field by its grain size, ranging from 3 mm to 25 cm, white weathered surface, and mineralogy consisting of essential feldspar, quartz, biotite and/or muscovite plus distinctive accessory minerals. Crudely defined zones were separated in the field based on the aerial variation and first appearance of specific accessory minerals in the pegmatites. As the supracrustal-pegmatite contact is -30- approached from the south, massive coarse grained to megacrystic pegmatite composed of quartz, plagioclase, microcline and biotite is first encountered. Red anhedral garnet occurs sporadically. Closer to the contact, felsic orthogneiss and paragneiss xenoliths are preserved and the pegmatite commonly exhibits well developed graphic intergrowths. Abundant garnet, muscovite, and fibrolitic sillimanite distinguish this zone. The sillimanite, retrograded to muscovite and quartz, occurs as fibrous mats and nodules with "feather-like" crystal habit (Photo 7a). The mats and nodules up to 15 cm in size, locally comprise up to 10 percent of the rock and occur isolated from each other or as interconnected "ropes" (Photo 7b). Within many nodules, the sillimanite appears to have nucleated from a central point. Alternatively, in a few of the nodules the fine sillimanite core is rimmed by coarse muscovite crystals intergrown with quartz. Both habits are inferred to have crystallized directly from magma (Percival et al. 1985). Percival et al. (1985) document identical sillimanite aggregates in granite pegmatite at Rainy Lake in Northwestern Ontario. They concluded that the feather-like clusters resulted from crystallization of a peraluminous magma suggesting a high liquidus temperature. Further, Percival equated the pegmatites and host granite to S-type granitoids of Chappell and White (1974) which are derived by anatexis from metasedimentary rocks. Pegmatite occurring adjacent to and as dikes intrusive into the supracrustal contain minor sulphides and tourmaline. Garnet and felsic metavolcanic and metasedimentary xenoliths are present -31- but sillimanite no©dules are absent. Tourmaline occurs as black crystals up to 5 cm long or as graphic intergrowths with quartz, the result of exsolution (Photo 8). Molybdenite is the principal sulphide in the pegmatite, however, pyrite is also present. White-weathering pegmatite also occurs as dikes and stocks in Scholfield and Caithness Townships. Mineral zonation is not evident in these bodies although sillimanite aggregates are common features. Emplacement of the stocks involved stoping of large metasedimentary blocks with attendant partial assimilation resulting in high grade metamorphic aureoles in the host rocks. The mineralogy and chemistry of the pegmatites when compared with the chemistry of spatially associated metasediments indicates a minimum melt composition is present in the pegmatites (Winkler, 1967). This suggests the pegmatites are anatectic, however, because there is no melanosome rimming gneissic xenoliths the pegmatites have moved from their place of origin. Application of the granitic pegmatite classification scheme summarized by Cerny, (1982) implies that anatectic pegmatites are not favoured hosts for rare-element (Li, Rb, etc.) deposits. Acceptance of this classification further implies the pegmatites formed at crustal depths of at least 7 to 11 km under almandine- amphibolite facies conditions (Winkler, 1967). Regional meta morphic patterns in the map area indicate the pegmatites have intruded greenschist facies rocks at a shallower crustal level than their depth of formation. East of Rufus Lake a granitic pegmatite intrudes mafic meta- volcanics and amphibolitic metasediments. The pegmatite is -32- composed of very coarse grained doubly terminated quartz crystals with plagioclase and potassium feldspar. Approximately 30 per cent of the rock is biotite in "books" averaging 5 cm long by 0.5 cm across. One phase of the pegmatite is megacrystic with potassium feldspar crystals up to 100 cm across and biotite "books" up to 70 cm long. The biotite has usually crystallized perpendicular to the surface of the outcrop and in cross section occurs as dendritic fans that have apparently nucleated along the contact of the megacrystic phase. Elsewhere in the map area, white-weathering pegmatite is generally absent. PROTEROZOIC AND ARCHEAN MAFIC INTRUSIONS DIABASE Diabase dikes intrude all rock types and three sets occur oriented approximately northwest, northeast and east-west. The northwest dikes are generally medium grained, brown weathering rocks that normally contain euhedral feldspar phenocrysts. However, feldspar phenocrysts are not evenly distributed within these dikes and in large exposures feldspar-bearing diabase was observed to grade into feldspar-barren diabase. This feature

combined with the poor exposure inhibits correlation of the dikes over long distance. Dikes containing feldspar phenocrysts are members of the Matachewan Swarm (cf. Watson, 1980, Thurston et al. 1977). In the Chapleau area a younger north-northwest set of feldspar barren diabase dikes assigned to the Mackenzie III swarm are recognized (Thurston et al. 1977) and it is possible unidentified members of this swarm are present in the map area. The northeast set of dikes are medium grained brown to dark -33- brown weathering. They are often magnetic but nonmagnetic members are common. Bennett et al. (1967) recognized this dike set and concluded its members were younger than the northwest dikes. The Abitibi Swarm is the most prominent northeast trend ing swarm of appropriate age in the map area (Watson, 1980), how ever, Thurston et al. (1977) recognized a northeast swarm in the Chapleau area that was not correlative with the Abitibi but was also younger than the Matachewan swarm. It is possible both swarms are in the map area and at least one dike intruding the Cargill carbonatite (Sage, 1983a) is younger than the complex (cf. Gittens et al. 1967). There are only a few members of the east-west dike set in the map area. These dikes weather dark brown and are always pervasively foliated subparallel to the dikes contacts. In one instance a dike is sinistrally offset by a northwest-trending fault and therefore predates at least one period of deformation. Bennett et al. (1967) and Thurston et al. (1977) did not recognize this dike set. It is suggested they represent the oldest diabase swarm in the map area and have undergone deformation. CENOZOIC QUATERNARY PLEISTOCENE AND RECENT

Much of the area is covered by a thin mantle of clay and clay-boulder till which effectively masks much of the bedrock geology. The larger river beds are at or near bedrock levels and judging from the incision of their banks overburden depth rarely exceeds 15 m in the map area. -34-

Pelletier, Scholfield, Doherty and part of Caithness Town ships are covered by post-Cochrane lacustrine sediments (Bennett et al. 1967). These deposits are tan to creamy white varved clays with minor silt and sand lenses. The rest of the area is covered by Cochrane Till (Bennett et al. 1967) which is composed of white to red clay-boulder till. A few eskers, kames and kettles composed of boulder till with minor sand layers comprise subordinate glacial features. Within the map area glacial striae record two major ice advance directions towards 195 O and 145 O azimuth. The latter ice direction clearly overprints the former direction and in many places the 195o glacial striae is preserved only on the lee of outcrops. Overlying the Pleistocene deposits are Recent sediments associated with swamps, lakes and rivers and are usually organic-rich. Petrochemistry Thirty samples representing the most abundant lithologies were selected for analysis (see Table 2). The data were plotted on a variety of diagrams in an attempt to characterize the rock types. QAP Diagram Figure 2 is a QAP diagram subdivided after Streckeisen (1976) and is used to classify the plutonic rocks. Within the map area there is a wide range of compositions with granodiorite the most common rock type. The Stray Lake Pluton is tightly constrained within the granodiorite field indicating homogeneous chemistry. This is -35- reflected in the field by the lack of variation in texture, weathering and colour of the outcrops. The felsic subvolcanic pluton northwest of Rufus Lake is also within the granodiorite field. There is a greater variation in proportions of plagioclase and alkali feldspar than in the Stray Lake pluton but generally the subvolcanic pluton has limited range of chemistry. This indicates that the various phases mapped in the field reflect textural differences as opposed to chemical changes within the pluton. The quartz-muscovite schist not shown on QAP plot (sample HK - 956, Table 2) is enriched in 5102 and 1^0 and depleted in CaO Na20 and A1203 compared to the subvolcanic pluton (samples HK-073 and HK-302, Table 2). This indicates the quartz-muscovite schist is not strictly the sheared equivalent of the plutonic rocks but has undergone hydrothermal alteration in conjunction with shearing. The significance of this alteration is not known, however, similar patterns have been observed in Red Lake gold deposits (Durocher, 1983) and in certain Abitibi gold deposits (Kerrich, 1983, Guha et al. 1982). On the QAP diagram the granitic pegmatites plot in the granite field. Although not abundantly represented on Figure 2, the pegmatites occupy a distinct area separate from the other plutons, which reflects the distinctive chemistry of these rocks. This is quite evident in the field as granitic pegmatites are distinctively white weathering and contain the crude mineral zonations previously discussed (see "General Geology", this report). -36-

The plutonic rocks within the gneissic terrane are multi- phased and range from tonalite to granite in composition. A consistent trend in these rocks is enrichment in alkali feldspar at the expense of quartz and plagioclase which may represent chemical evolution of the plutons. Alternatively potassium meta somatism may explain the observed trend and there is field evidence in the form of alkali feldspar veinlets that favour this process though the true granite phases show no sign of potassium metasomatism. Lastly, the QAP diagram effectively characterizes the monzonite intrusion in Pelletier Township and indicates its quartz-deficient nature. Different phases were not recognized in the field. It is only through plotting the data on the QAP diagram that the wide spread in composition is apparent. Data for the QAP diagram were derived from petrographic analysis of hand samples and thin sections (point counting and feldspar staining). This method is preferred to the use of normative calculations because it is quicker and represents modal proportions. For example sample MH-009 (Table 2), a monzonite from Pelletier Township was examined petrographically and no quartz was observed either in hand sample or in thin section. A portion of the same sample was analyzed and the resulting data used to derive normative rock compositions. Three normative calculations: Barth-Niggli cation Norm, CIPW norm, and the Barth Mesonorm for granitic rocks, indicate sample MH-009 is quartz normative, at variance with modal data. A second example indicating the discrepancy between modal -37- and normative calculations involves sample HK.-073 (Table 2) representative of subvolcanic pluton. Petrographic examination following the same procedures, indicates HK-073 is a granodiorite yet normative calculations suggest the rock is a granite. CaO - Na20 - K20 Diagram Figure 3 is the CaO-NaaO-I^O Diagram for the Hearst- Kapuskasing area and shows the range of mafic metavolcanics, felsic metavolcanics and metasediments for these chemical components. This ternary system (as used by Condie, 1967) is useful to illustrate the likely provenance of the clastic meta sediments in the map area. The overlapping felsic metavolcanic and metasedimentary fields indicate a chemical affinity between the two rock types and that the felsic metavolcanics provided much of the detritus now preserved in the metasediments. There appears to have been very little contribution by the mafic meta volcanics. Similar trends are observed in other greenstone terranes (Ojakangas 1985, Berger 1981) and the inference is that the volume of erupted felsic metavolcanics was much greater than is now preserved in the map area (Thurston et al. 1985). AFM Diagram The AFM diagram (Figure 4) is commonly used for metavolcanic rocks. It was originally intended (Irvine and Baragar, 1971) to distinguish solely between tholeiitic and calc-alkaline basalts; however, plotting all metavolcanic rock types on the diagram, as in this report, often emphasizes specific chemical trends. Figure 4- shows that all analyzed mafic metavolcanics are tholeiitic basalts. -38-

The felsic metavolcanics are generally calc-alkaline and show a wide range of composition. The sample of felsic meta- volcanic plotting in the tholeiitic field appears to have abnormal chemistry which is emphasized by Figure 4-. This sample, HK-027 (Table 2) contains S102 and MgO levels compatible with the other felsic metavolcanics in the area but contains total iron, T102 and K20 levels more compatible with the basalts. Although the rock was mapped as a basalt it was thought to represent the extrusive equivalent of the hornblende monzonite in Pelletier Township so elevated S102 * s not unexpected. Further work is required in this area to determine whether the rock is altered or a true extrusive equivalent of the monzonite intrusion.

Si0 2 vs. Na20 * K20 Diagram Figure 5 is presented for two purposes. Firstly it demonstrates the subalkaline nature of all the metavolcanics which is a prerequisite for use of the Jensen Cation Plot, Figure 6 (Jensen 1976). Secondly the diagram shows the strong bimodal character of metavolcanics in the map area a subject which will be discussed later. Alkalis are susceptible to alteration and regarded as unreliable for chemical classification (Church, 1975). The tightly constrained mafic metavolcanic field on Figure 5 suggests alkali mobility is not a major problem, although it may be locally important within the map area. Alkali mobility would be expected to scatter data as intensity of alteration varied throughout the affected areas. Jensen Cation Plot -39-

The jensen Cation Plot, Figure 6, is commonly used to classify subalkalic volcanic rocks (Jensen 1976). The plot has the added advantage of classifying felsic as well as mafic volcanics. Mafic metavolcanic rocks in the map area vary between high- iron tholeiites and high magnesium tholeiites. The fairly tight clustering of data indicates there has been little differentia tion in major oxide chemistry. The Oensen Cation Plot provides a further means of distinguishing rock types based on colour. With regards to the mafic metavolcanics this classification works well as most rocks are dark green to black on fresh surface in correspondence with their chemical classification. The felsic metavolcanics plot as calc-alkaline rhyolites and dacites. As with the mafic metavolcanics, there is a close correspondence between chemical composition and colour for the rhyolites and dacites which are white to buff on fresh and weathered surface. The importance of colour correspondence indicates chemistry of individual outcrops can be implied in the field, if the metamorphic grade is known, without recourse to analysis and immediately provides a useful exploration guide. The Oensen Cation Plot Figure 6 shows a well defined bimodal distribution of the metavolcanic rocks. This is a common feature in many Archean greenstone terranes throughout the world (Thurston et al. 1985). The implications of a bimodal distribution are many and insufficient detailed mapping and geo chemistry is presented herein to provide definitive conclusions at this time. If the quartz-plagioclase-epidote concentrations -40- in the centers of many pillow forms are coalesced varloles then bimodal volcanism of the type envisaged by Thurston et al. (1985) may have operated in the area. Bimodal volcanism as defined by Thurston et al. (1985) implies production of large volumes of felsic magma. Although there are only small volumes of felsic metavolcanics preserved in the map area the provenance of the clastic metasediments (Figure 3) indicates a greater volume of felsic material once existed which is compatible with bimodal volcanism. The extreme bimodal distribution of the metavolcanics is interpreted to result from separate magma sources; however, more work is required to prove this statement. STRUCTURAL GEOLOGY Summary The limited amount of outcrop precludes a detailed structural analysis; however, polyphase deformation has affected the entire map area and is most evident in the supracrustal rocks. At least two phases of deformation are recognized with the older, D-j deformation characterized by east-trending fold axes and lineations. Throughout the central and southern parts of the supracrustal belt east-trending folds are deformed by conjugate northeast and northwest crenulation cleavages and by northeast trending fold axes. This younger deformation (03) is characterized by northeast trending folds, lineations and transposition of bedding and DI folds. First Deformation (Di) The supracrustals are generally south facing but local reversals indicate folding has occurred. This folding event is the oldest preserved in the map area and is characterized by east-trending fold axes with shallow plunges. The folds, of which the syncline in northern Scholfield and Caithness Townships is an example, are isoclinal with steeply dipping axes and limbs. Small and large scale fold closures contain greater concentrations of quartz veining than the limbs and in many places the veins are also folded. Locating the positions of large scale fold closures is best accomplished by using the vergence of small scale structures as bedding-cleavage relation ships cannot be used because the two are often parallel. Small scale fold axes most often define the DI lineation (Photo 9) and mineral lineations are less frequent. First deformation folds are best preserved in the northern part of the map area, west of Ecclestone Township. Elsewhere, D-j folds are destroyed or overprinted by subsequent deformation, intrusion and metamorphism. Second Deformation (03) There is abundant evidence in the supracrustal rocks that a second deformation (02) has affected the map area. Interference fold patterns (Photo 10) clearly show northeast and complementary northwest fold axes were developed. Moderate to shallow plunging mineral lineations are well developed in the rocks; however, the D2 cleavage occurs as spaced fractures and is poorly developed. A common 03 feature is transposition of units in fold closures (Photo 11). Recognition of transposition is important because it prohibits development of a reliable stratigraphy. -42-

Locally sulphide mineralization occurs in shear zones or faults that result from extreme transposition. This is most commonly observed between Fergus and Flatt Lakes where transposed iron stone beds create the impression that multiple horizons exist when, in fact, relatively few ironstone horizons are present. Northeast-trending shear zones that locally host sulphides situated in the felsic subvolcanic pluton south of Flatt Lake are related to the same event. Brittle deformation occurs along the Rufus Lake Fault in the east part of the map area. The fault records a complex history of movement but is principally a 03 feature because northeast- plunging slickensides parallel to D2 lineations are preserved on the fault plane and subsidiary shears in the supracrustals locally occupy axial planes of northeast-trending folds. There are no definitive marker horizons displaced across the fault but the deflection of foliations and schistosities indicates a component of dextral transcurrent movement occurred. The Juxtaposition of metasediments and gneiss plus a prominent fault scarp on Rufus Lake indicate significant vertical movement on the fault with the east block on the upthrown side. These observations are in general agreement with Percival (1985) who studied the Moonbeam area, northeast of Rufus Lake and indicates D2 is a regional event. As previously mentioned diabase dikes exploited existing structural weaknesses. The principal dike sets are aligned parallel the D2 fold axes and are usually undeformed which indicates post tectonic intrusion. In two places on the -43-

Opasatika River; however, the Rufus Lake Fault is occupied by sheared and hydrothermally altered diabase which suggests reactivation of the fault after diabase intrusion. This implies the Rufus Lake Fault has had a long and complex history of movement. Approximately 6 km east of the Rufus Lake Fault a large diabase dike strikes northeast through the map area. This dike occupies a fault which cuts the Cargill carbonatite east of the map area (Sage 1983a) and is regional in extent. The dike is undeformed and appears to have passively intruded along the fault plane. This structure is important as it is implied by previous workers (Percival, 1985; Watson, 1980, Bennett et al. 1967) to be involved with the development of, or marks the boundary of the Kapuskasing structure. METAMORPHISM In determining metamorphic conditions prevalent in the map area, emphasis was placed on textures in the pelitic meta- sediments. Regional metamorphism in the map area ranges from middle to upper greenschist facies (ref. Winkler 1967). The diagnostic minerals in the metasediments are garnet, probably almandine, and blue-green hornblende in coexistence with actinolite in more mafic wackes. In the mafic wackes blue-green hornblende is a common constituent and hornblende crystals are occasionally cored by actinolite. Winkler (1967) regards this relationship as diagnostic of greenschist metamorphism because actinolite disappears under higher grade conditions. Alone, garnet is not a reliable indicator of greenschist metamorphism as it develops at low grade and persists to very high grade conditions in rocks of appropriate composition (Winkler 1967). In the map area, how ever, garnet is common in all rock types and this is considered by the author to indicate metamorphic conditions compatible with upper greenschist facies. Supporting mineralogical evidence for upper greenschist metamorphic conditions include metamorphic plagioclase with An content greater than 30 and stable coexistence of chlorite in the presence of quartz (Winkler 1967). In general the absence of staurolite and the paucity of cordierite in rocks of appropriate composition indicates amphibolite rank metamorphic conditions were not attained in most of the supracrustals. Amphibolite rank conditions, however, affected supracrustal rocks in the west and southwest parts of the map area as indicated by the presence in metasediments of sillimanite, staurolite and cordierite with lesser amounts of cummingtonite and microcline. Amphibolite rank supracrustals are spatially restricted to the peripheries of the granitic pegmatite plutons, and this suggests the intrusions imposed contact thermal metamorphism upon these rocks. The absence of chlorite, except as a retrograde phase, in most mineral assemblages is further evidence that amphibolite rank metamorphism prevailed around the borders of the plutons. Mineral assemblages in the pelitic metasediments along with field relationships constrain metamorphic conditions in the map area. The onset of amphibolite rank metamorphism is marked by -45- the first appearance of staurolite and cordierite and the disap pearance of chlorite from metasediments (Winkler 1967). Staurolite is absent in most metasediments and cordierite is only poorly developed in rocks spatially unrelated to the pegmatitic plutons. Myashiro (1973) and Winkler (1967) indicate cordierite can form at temperatures between 500 0C to 535 0 C between 2 and 4 kbar pressure and staurolite forms at 540oc at 4 kbar. It is suggested the lower temperature conditions prevailed over most of the supracrustal assemblages. The coexistence of cordierite and almandine limits metamorphic pressure as cordierite forms under low to moderate pressure and almandine forms under moderate to high pressure. Winkler (1967) estimates cordierite cannot be formed above 5.3 kbar at 600 OC and clearly the presence of any cordierite in the metasediments indicates these conditions were not exceeded in the supracrustals. Myashiro (1973) notes that as pressure increases the abundance of almandine increases and cordierite is restricted to rocks with specific bulk compositions. Given the field evidence it appears moderate pressures, estimated between 4 to 5 kbar (14-17.5 km depth) operated in the map area (cf. Percival and Card, 1985). The metasediments of amphibolite rank contain characteristic assemblages observed elsewhere in the Quetico Subprovince (Pirie and Mackasey 1978). These assemblages provide good pressure and temperature constraints. The mineral assemblage biotite - garnet - cordierite - staurolite - sillimanite (fibrolite) occurs in Doherty Township and sets a minimum temperature of 550 O C and -46- pressure of 3.2 to 4.8 kbar (Pirie and Mackasey 1978). The assemblage biotite - muscovite - sillimanite with trace garnet is the most common assemblage and in west-central Doherty Township biotite - K-feldspar-garnet - muscovite occurs nearby. These represent the maximum metamorphic conditions without significant partial melting and correspond to 700 0C at 4 kbar (Pirie and Mackasey 1978). Field relationships indicate the granitic pegmatite intrusions formed by anatexis of the metasediments and felsic metavolcanics and by extension of the evidence above, must have formed at temperatures exceeding 700oc. From experiment, Winkler (1967) observed that the breakdown of muscovite in the presence of quartz occurred at 725oc at 5 or more kbar. Muscovite and quartz yield a melt containing potassium feldspar, quartz and a residuum of sillimanite and quartz. If the sillimanite forms aggregates the rock formed upon crystallization is composed of potassium feldspar, quartz and sillimanite aggregates surrounded by quartz similar to the granitic pegmatites (Winkler, 1967). Therefore, 725 O C and 5 kbar represent the minimum conditions under which the granitic pegmatites formed. This supports the concept that the pegmatites were emplaced at shallower crustal levels than their depth of formation. Metamorphism in the gneissic terrain is difficult to characterize because there are few indicator minerals and the felsic domes interrupt any patterns that may have developed. Generally, hornblendes in the gneiss are green to blue green in thin section suggesting higher temperatures than affected the -47- supracrustals. The amount of felsic mobilizate in the gneisses increases further south in the map area. For these reasons upper greenschist to amphibolite rank metamorphism is assumed to have affected the gneisses. A serious problem regarding metamorphism in the map area is the absence of andalusite in the metasediments. Given the pressure and temperature conditions inferred, andalusite should be common in the metasediments. The reasons that it was not observed anywhere can not be satisfactorily explained and further work is required. Among the possible explanations, inadequate sampling is least likely as a large number of representative samples of metasediments were specifically collected for meta morphic study. The role of bulk chemistry of the metasediments is uncertain but it seems that if observed sillimanite can form in certain wacke beds andalusite should be present in similar wacke beds of lower metamorphic grade and therefore its absence is a situation open for further study. ECONOMIC GEOLOGY The history of mineral exploration in the map area is minimal and there is no record of recent activity using modern exploration techniques and concepts. Although economic mineral occurrences are unknown the potential exists for their discovery. The Cargill Township phosphate-vermiculite deposit (located east of the present map area), under option to Sherritt Gordon Mines Limited, is hosted by carbonatite (Sage, 1983a). Initial exploration of the deposit by Continental Copper Mines Limited in -48-

extended westward into Ecclestone Township but subsequent exploration efforts have been centered on the intrusion. Several sulphide-bearing samples were collected during the 1985 field season and submitted to the Geoscience Laboratories, Ontario Geological Survey, for analysis (Table 3). One sample consisting of sulphide fragments picked from a mafic debris flow in Ecclestone Township returned an assay of 160 ppb Au which is elevated above normal background levels of 10 to 70 ppb for Archean sulphide schists (Boyle, 1976). The remaining samples did not return assays significantly above background levels for any element analyzed. DESCRIPTION OF PROPERTIES Robert Campbell Property [1960] (1) Trenching and diamond drilling was carried out in the north east corner of Lot 17, Concession II of Caithness Township by Robert Campbell in 1960. Two diamond drill holes totalling 205 feet (62.5 m) were collared to intersect a northeast-trending mineralized shear zone. The drill logs, on file with the Resident Geologist©s Office, Ministry of Northern Development and Mines in Timmins, indicate quartz, pyrite and pyrrhotite were intersected in sheared "greenstone". No assays were reported and the claim was allowed to lapse. Neither trenches nor diamond drill holes were located during the mapping. Kenogamisis Gold Mines Limited [1965] (2) In 1964 Kenogamisis Gold Mines Limited acquired, by staking, 50 unpatented claims in Ecclestone and Parnell Townships east of the Opasatika River. Ground horizontal loop electromagnetic and -49- magnetic surveys were carried out on cut lines over 40 of the claims. A number of electromagnetic conductors and magnetic anomalies were outlined by the surveys and seven diamond drill holes totalling 1761 feet (537 m) tested selected targets. Pyrite and pyrrhotite were encountered in each hole in association with quartoze gneissic rock. Subordinate rock types include amphibolitic gneiss, feldspar porphyry and quartz- sericite schist with green mica and carbonate minerals reported in two of the holes. No assays were reported and the property was subsequently dropped. Macassa Mines Limited [1960] (3) In 1960 Macassa Mines Limited optioned 49 unpatented claims in Caithness and Doherty Townships staked by Lundberg Explorations Limited in 1959. These claims covered the north halves of Lots 11, 12, 13, 14 and 15 of Concession I, the south halves of Lots 15, 16 and 17 of Concession 2, the south halves of Lots 11, 12, and 13 of Concession 3, all of lots 16 and 17, Concession 1 and all of Lots 11, 12, 13 and 14 of Concession 2. Macassa Mines Limited carried out ground electromagnetic (Turam) and magnetic surveys to follow up the airborne electro magnetic and magnetic surveys carried out by Lundberg Explorations Limited in 1959. Four northeast-trending conductors were outlined by the ground surveys and these were interpreted by the geophysical contractor to be caused by shear zones mineralized with sulphides or graphite. Personnel employed by Macassa Mines Limited collected samples of rusty rock containing disseminated magnetite, pyrite and pyrrhotite. These samples -50- returned assays of Nil gold and Nil to .02 ounce per ton silver. Macassa Mines Limited did no further work on the claims and allowed them to lapse. Steve Vukmiromich [1980] (4) Steve Vukmiromich drilled four diamond holes totalling 443 feet (135 m) on three claims in Caithness Township. Three of these holes totalling 342 feet (104 m) were drilled south of Big Pike Lake on Lots 5 and 6, Concession 2 in respectively 1974, 1976 and 1977. Each hole encountered rock interpreted by the author, to be mafic metavolcanics or diorite. Minor amounts of quartz, epidote and pyrite were reported in each hole. In 1980, one diamond drill hole (101 feet, 30.8 m) was collared on Lot 16, concession 2 in Caithness Township. The location of the hole corresponds approximately to one of the ground electromagnetic conductors outlined by Macassa Mines Limited in 1960. "Pyroxene", quartz and pyrrhotite were encountered in the hole. No assays were reported from any of the holes and the claims were allowed to expire. Mike Wabano (5) In 1980 Mike Wabano sunk several trenches on a claim in Lot 13, Concession 2 in Caithness Township. This area was previously explored by Macassa Mines Limited in 1960 and presumably the trenches, which were not found in 1985, are located near ground electromagnetic conductors previously outlined. No record of rock type or assays were reported by Mr. Wabano but outcrops examined during the 1985 field season suggest that mafic -51- metavolcanic rocks were trenched. RECOMMENDATIONS FOR FUTURE EXPLORATION Future exploration should concentrate on the metavolcanic rocks and to a lesser extent on the spatially associated meta- sedimentary rocks, pegmatites and gneisses. Clay overburden covering most of the area is commonly less than 15 m thick which facilitates use of conventional airborne and ground geophysical methods to trace hidden lithologic units and electromagnetic conductors. Soil, humus and lithogeochemistry applied selectively as conditions warrant could be useful over the metavolcanics where outcrop is more abundant and overburden is thinner. Recognition of the northeast-trending and complementary northwest-trending D2 structures is important as transposition of units and localiza tion of sulphides in resultant faults and shear zones can occur. There are five major environments which could host economic mineral deposits in the map area. These are: 1) felsic metavolcanics 2) structural, eg. faults and shear zones 3) ironstone 4) debris flow and intermediate pyroclastics and 5) pegmatite 1) Felsic Metavolcanic Environment The area of Pelletier and Doherty Townships underlain by felsic pyroclastics is a favourable target for volcanogenic massive sulphide deposits. Randomly dispersed sulphide fragments in the pyroclastics indicate ore forming processes may have -52- occurred. The presence of microscopic tourmaline in the under lying metasediments suggests that widespread boron metasomatism may have been the result of hydrothermal activity in the south- west part of the supracrustal. The rhyolite to trachyte flows in the north part of Fergus Township are poorly exposed and unexplored. The flows may be more extensive than mapped and a major felsic metavolcanic sequence may be present along the northern boundary of the map area. The subvolcanic felsic pluton northwest of Rufus Lake is spatially associated with sulphide-bearing intermediate tuffs and ironstones. In this environment gold and base metal mineral ization is possible. 2) Structural Environment The Rufus Lake fault is a major structural feature in the map area and may be regional in extent. Where the fault cuts the subvolcanic felsic pluton quartz-muscovite schist is developed and pyrite plus epidote-bearing quartz veins have intruded parallel to the fault plane. The quartz-muscovite schist is an important subunit as gold is often found hosted by this rock type in other greenstone terrains. The schistose structure of this unit developed by shearing and at least some of the muscovite has developed by potassium metasomatism. The Rufus Lake fault was formed during the second deformation. The spatial association of sulphides with the fault means that northeast-trending structures are important exploration targets. -53- 3) Ironstone Environment

Numerous sulphide-oxide facies ironstones occur throughout the map area. Pyrite, pyrrhotite, graphite and magnetite with trace amounts of chalcopyrite are common in most showings. Ironstones are indicative of an exhalative environment and many base and precious metal deposits are spatially associated with these rocks in other greenstone terrains. One of the more extensive ironstone occurrences is in Pelletier Township approximately 600 m north of forestry access road 25-8-14. A folded succession of mafic tuffs and pyritic ironstone is exposed over an area 250 m by 1000 m. Well developed gossan marks the ironstone and extensive sampling is warranted (Photo 6).

In Caithness Township, 800 m west of the Mattiwitchewan River a massive sulphide facies ironstone is exposed. A three meter thick succession of rusty mafic tuffs, chert, massive pyrrhotite and massive graphite is interbedded with wackes. Random grab samples (numbers HK 925, 926, 927, 928, Table 3) returned low assay values but the strike extension is overburden covered and remains unexplored. 4) Debris Flow and Intermediate Pyroclastic Environment Intermediate pyroclastics interlayered with debris flows underlie the central parts of Ecclestone and Rykert Townships. The debris flows contain mafic clasts, chert and sulphide fragments and locally the sulphides contain up to 160 ppb Au (sample HK-534, Table 3) which indicates the potential for gold concentration in this environment. The chert and sulphide -54- fragments are assumed to have originally been components of ironstone beds or massive sulphides incorporated into debris flows by avalanching from volcanic edifices. Future exploration should be directed towards discovery of sulphide mineralization in a proximal volcanic environment. Further, the intermediate pyroclastics in Ecclestone Township are similar to those in Rykert Township suggesting the intervening area where pyroclastics are apparently absent warrants further examination. In particular the cause of the large aeromagnetic high outlined on ODM-GSC Map 2237G (1963c) may be economically important if volcanic or plutonic rocks underlie the area. 5) Pegmatite Environment The white weathering pegmatites in the west and southwest part of the map area were derived by anatexis of the meta- sediments and felsic metavolcanics. Boron and sulphides originally present in the supracrustals were apparently incorporated into the anatectic magmas and recrystallized as tourmaline, molybdenite and pyrite in pegmatites adjacent to and intrusive into the supracrustal rocks. Anatectic pegmatites are not favoured hosts for rare element deposits (Cerny, 1982), how ever, economic concentrations of molybdenum and any other element incorporated into the magmas could be present in this environment. Additionally, the presence of sillimanite aggregates formed by crystallization from the magmas indicates the pegmatites were derived from peraluminous melts. Together with their anatectic -55- origin these pegmatites show strong affinity to S-type granitoids (Chappeil and White, 1974) which are preferred hosts for tin, tungsten and fluorine deposits and it is recommended the pegmatites be examined for these minerals. -56-

References American Geological Institute 1980: Glossary of Geology; Edited by R.L. Bates and 3.A. Jackson, 74-9p. Ayres, L.D. and Thurston, P.C. 1985: Archean Supracrustal Sequences in the Canadian Shield: An Overview; p.34-3-380 In Evolution of Archean Supracrustal Sequences, edited by L.D. Ayres, P.C. Thurston, K.D. Card, W. Weber, Geological Association of Canada Special Paper 28, 380p. Ayres, L.D. and Cerny, P. 1982: Metallogeny of Granitoid Rocks in the Canadian Shield; The Canadian Mineralogist, Vol.20, p.4-39-536. Bell, Robert 1877: Report on an Exploration in 1875 between Games Bay and Lakes Superior and Huron; Geological Survey of Canada Report of Progress 1875-76, p.294--342. Bennett, G., Brown, D.D., George, P.T., Leahy, T. 1967: Operation Kapuskasing; Ontario Department of Mines, Miscellaneous Paper 10, 98p. Accompanied by maps P.397 and P.398, scale 1:127 520. Berger, B.R. 1981: Stratigraphy of the Western Lake St. Joseph Greenstone Terrain, Northwestern Ontario; Unpublished M.Se. thesis, Lakehead University, Thunder Bay, Ontario. 117p., 2 appendices, 3 maps. -57-

Borradaile, G.O., Bayly, M.B., and Powell, C.McA. 1982: Atlas of Deformatlonal and Metamorphic Rock Fabrics; Sprlnger-Verlag Berlin, Heidelberg (Printed in Germany, 551p.). Boyle, R.W. 1976: Mineralization Processes in Archean Greenstone and Sedimentary Belts; Geological Survey of Canada, Paper 75-15, 45p. Brown, M. 1973: The Definition of Metatexis, Diatexis and Migmatite; Proceedings of the Geologist©s Association, Vol.84, Part 4, p.371-382. Card, K.D. 1982: Progress Report on Regional Geological Synthesis, Central Superior Province; p.23-28, In Geological Survey of Canada, Current Research Part A, Paper 82-1A. Card, K.D., Percival, 3.A., Lafleur, 0., Hogarth, D.D. 1981: Progress Report on Regional Geological Synthesis, Central

L Superior Province, p.77-93 In Geological Survey of Canada Current Research Part A, Paper 81-1A. Card, K.D., Percival, 3.A., Coe, K. 1980: Progress Report on Regional Geological Synthesis, Central Superior Province; p.61-63. In Geological Survey of

Canada Current Research Part A, Paper 80-1A. Cerny, P. 1982: Anatomy and Classification of Granitic Pegmatites; p..1-39 in Granitic Pegmatites in Science and Industry Edited by -58-

P. Cerny, Mieralogical Association of Canada, Short Course Handbook, Vol.8. Chappell, B.W., White, A.3.R. 1974: Two Contrasting Granite Types; Pacific Geology, Vol.8, p.173-174. Church, R.N. 1975: Quantitative Classification and Chemical Comparison of Common Volcanic Rocks; Geological Society of America Bulletin, Vol.86, p.259-263. Condie, K.C. 1967: Geochemistry of Early Precambrian Graywackes from Wyoming; Geochimica et Cosmochimica Acta Vol.31, p.2135-2149. Durocher, M.E. 1983: The Nature of Hydrothermal Alteration Associated with the Madsen and Starratt-Olsen Gold Deposits, Red Lake Area; (p.123-140) In The Geology of Gold in Ontario, edited by A.C. Colvine, Ontario Geological Survey; Miscellaneous Paper 110, 278p.

Fahrig, W.F., Gaucher, E.H., Larochelle, A. 1965: Paleomagnetism of Diabase Dikes of the Canadian Shield; Canadian Journal of Earth Science, Vol.2, p.278-298. Geological Survey of Canada 1903-05: Geological Map of portions of the Districts of Algoma and Thunder Bay by Wilson, W.5, Collins, W.H., Scales 1 inch to 8 miles or 1:506,880. Gittins, 0., Maclntyre, R.M., York, D. 1967: The Age of Carbonatite Complexes in Eastern Canada; -59-

Canadian Journal of Earth Sciences, Vol.4, p.651-655. Guha, J., Gauthier, A., Vallee, M., Descarreaux, 0., Lange-Brard, F. 1982: Gold Mineralization Patterns of the Doyon Mine (Silverstock), Bousquet, Quebec; p.50-57 in Geology of Canadian Gold Deposits, edited by R.W. Hodder and W. Petruk, Special Volume 24, Canadian Institute of Mining and Metallurgy, p.286. Hatch, F.H., Wells, A.K., Wells, M.K. 1972: Petrology of the Igneous Rocks, Thomas Murby and Company, 40 Museum Street, London, W.C.1, 551p. Irvine, T.N., and Baragar, W.R.A. 1971: A Guide to the Chemical Classification of the Common Volcanic Rocks; Canadian Journal of Earth Science, Vol.8, p.523-548. Jensen, L.S. 1976: A New Cation Plot for Classifying Subalkalic Volcanic Rocks; Ontario Division of Mines, Miscellaneous Paper 66, 22p. Kerrich, R. 1983: Geochemistry of Gold Deposits in the Abitibi Greenstone Belt; The Canadian Institute of Mining and Metallurgy, Special Volume 27, 75p. Macdonald, G.A. 1972: Volcanoes; Printice-Hall Incorporated, Inc. Englewood Cliffs, New Jersey, 510p. McGlynn, 3.C. -60-

1970: Geology of the Canadian Shield; pp.54-119, In Geology and

Economic Minerals of Canada, Geological Survey of Canada, Economic Geology Report No.1, edited by R.3.W. Douglas, 838p. Mehnert, K.R. 1968: Migmatites and the Origin of Granitic Rocks Elsevier Publishing Company, Amsterdam, London, New York, 393p. Miyashiro, A.

1973: Metamorphism and Metamorphic Belts; George Allen & Unwin Limited, London, 492p. Ojakangas, R.W. 1985: Review of Archean Clastic Sedimentation, Canadian Shield: Major Felsic Volcanic Contributions to Turbidite and Alluvial Fan-Fluvial Facies Associations; p.23-47, In Evolution of Archean Supracrustal Sequences, edited by Ayres, L.D. Thurston, P.C. Card, K.D. and Weber, W. Geological Association of Canada Special Paper 28, p.380. Ontario Department of Mines - Geological Survey of Canada 1963a: Aeromagnetic Map 2223G - Goat River, Algoma and Cochrane Districts, Ontario, Scale 1 inch to 1 mile or 1:63,360. 1963b: Aeromagnetic Map 2224G - Mead, Algoma and Cochrane Districts, Ontario, Scale: 1 Inch to 1 mile or 1:63,360. 1963c: Aeromagnetic Map 2237G - Opasatika Lake, Algoma and Cochrane Districts, Ontario, Scale: 1 inch to 1 mile or 1 :63,360. 1963d: Aeromagnetic Map 2238G, Magladery Creek, Algoma and Cochrane Districts, Ontario, Scale: 1 inch to 1 mile or -61- 1:63,360. 1963e: Aeromagnetic Map 2251G; Woman Falls, Algoma and Cochrane Districts, Ontario, Scale: 1 inch to 1 mile or 1:63,360. 1963f: Aeromagnetic Map 2252G - Lost River, Algoma and Cochrane Districts, Ontario, Scale: 1 inch to 1 mile or 1:63,360. Percival, 3.A. 1985: The Kapuskasing Structure in the Kapuskasing Fraserdale Area, Ontario; p.1-5, In Current Research, Part A, Geological Survey of Canada, Paper 85-1A. Percival, 3.A., Stern, R.A., Digil, M.R. 1985: Regional Geological Synthesis of Western Superior Province, Ontario; p.385-397, In Geological Survey of Canada, Paper 85-1A, Current Research Part A. Percival, 3.A., Card, K.D. 1985: Structure and Evolution of Archean Crust in Central Superior Province, Canada; p.179-192; In Evolution of Archean Supracrustal Sequences edited by L.D. Ayres, P.C. Thurston, K.D. Card, and W. Weber; Geological Association of Canada, Special Paper 28, 380p. Percival, 3.A., Card, K.D. 1983: Archean Crust as Revealed in the Kapuskasing Uplift, Superior Province, Canada; p.232-326, Geology, Vol.11. Pirie, 3., Mackasey, W.O. 1978: Preliminary Examination of Regional Metamorphism in Parts of Quetico Metasedimentary Belt, Superior Province,

Ontario; p. 37-4-8 In Metamorphism in the Canadia Shield, Geological Survey of Canada; Paper 78-10, edited by 3.A. -62-

Fraser, W.W. Heywood, 367p. Sage, R.P. 1983a: Geology of the Cargill Township Carbonatite Complex; Ontario Geological Survey Open File Report 5400, 46p., 2 tables, 2 figures, 1 appendix and 1 map in back pocket. 1983b: Literature Review of Alkalic Rocks - Carbonatites: Ontario Geological Survey, Open File Report 5436, 277p., 1 photo. Spry, Alan 1969: Metamorphic Textures; Pergamon Press, Toronto, 350p. Streckeisen, A. 1976: To Each Plutonic Rock its Proper Name; Earth-Science Reviews, Vol.12, p.1-33. Thurston, P.C., Ayres, L.D., Edwards, G.R., Gelinas, L., Ludden, O.N., Verpaelst, P. 1985: Archean Bimodal Volcanism in "Evolution of Archean Supracrustal Sequences", p.7-21, edited by L.D. Ayres, P.C. Thurston, K.D. Card and W. Weber; Geological Association of Canada Special Paper 28, 380p. Thurston, P.C., Siragusa, G.M., Sage, R.P. 1977: Geology of the Chapleau Area, Districts of Algoma, Sudbury, and Cochrane; Ontario Division of Mines, GR157, 293p., accompanied by Map 2351, 2352, scale 1:250,000 and map 2221, scale 1 inch to 4 miles (1:253,440). Walker, R.G. 1979: Facies Models, Toronto, Geological Association of Canada, 211p. Watson, 3. -63-

1980: The Origin and History of the Kapuskasing Structural Zone, Ontario, Canada; Canadian Journal of Earth Science, Vol.17, p.866-875. White, A.O.R. and Chappell, B.W. 1983: Granitoid Types and their Distribution in the Lachlan Fold Belt, Southeastern Australia; Geological Society of America, Memoir 159, p.21-34. Williams, H., and McBirney, A.R. 1979: Volcanology; Freeman, Cooper A Co., San Francisco, 397p. Winkler, H.G.F. 1967: Petrogenesis of Metamorphic Rocks. Revised Second Edition, Springer-Verlag, New York Inc., 220p. -64-

LOCATION MAP Scale: 1:1 548 000 or 1 inch to 25 miles

FIGURE 1. Location Map, Hearst-Kapuskasing Area. -65-

QUARTZ

X Monzonite M Stray Lake Pluton A Subvolcanic pluton 9 Felsic plutons intruding gneiss O Granitic pegmatite

(after Streckeijen . 1976)

FIGURE 2. -66-

CaO

No 2O K2 0

m Mafic Metavolcanics x Metasediments A Felsic Metavolcanics

( after Cond i e. 196 7 ) FIGURE 3 -67-

No2O * K2O MgO

x Mafic Metavolcanics A Felsic M etavolcanics

after Irvine and Baragar 1971)

FIGURE 4 -68-

49.5 52.5 70.5 73.5 Sio2

FIGURE 5 -69-

F03+F02+T!

Mg

After J ensen 1976

FIGURE 6 - 70 -

Photo 1: Well formed pillow In basalt from outcrop at Junction of Synco Road and Caithness Forest Access Road. Interselvage material composed of resistant weathering hornblende and epidote. Pillow Is south facing toward top of photograph. Hammer Is 35 cm long.

Photo 2a: Intermediate pyroclastic breccia. Felsic clasts (light colour) in mafic matrix may indicate epiclastic origin. West-central Ecclestone Township (3.5 km west of Opasatika River. Compare with Photo 2b. - 71 -

— ~- " v *i "™"M*:n; ""'i — —^•^•••^•••pBw^ji.i - flmW- w*~'T'fdHHHHV^ * ' Photo 2b; Heterolithic Intermediate pyroclastic breccia composed of felsic clasts (light colour) and mafic clasts (dark grey) in a mafic tuffaceous matrix. Pelletier Township 500 m north of forest access road 25-8-1*.

Photo 3a: Quartz "eyes" (QTZ) and felsic, clasts are characteristic of the felsic pyroclastics in Pelletier and Doherty Townships. Photo taken from outcrop along side of logging road in west part of Doherty Township. -72-

Photo 3b: Quartz "eyes" (QTZ) and clasts (C) are still recognizable In tectonlcally deformed felsic pyroclastics. Sheared matrix is composed of muscovite and quartz. Photo taken on fores access road 25-8-5 In northeastern Doherty Township.

Photo *: Crenulated quartz-muscovite schist developed by shearing and alteration of quartz-feldspar porphyry of the subvolcanic pluton. Photo taken along road on northwest side of Rufus Lake. -73-

Photo 5: Typical bedded wackes showing variation In bedding styles. Beds under hammer are graded showing tops to south (right side of photo). Note transposing cleavage which disrupts some of the beds. Photo taken In northern Rykert Township. Hammer Is 35 cm long.

Photo 6: Deformation of Ironstone created tectonlcally thickened sequences located 800 m north of forest access road 25-8-1* In Pelletier Township. Fold closure Is approximately due west. -74-

Photo 7a: Isolated flbrolitlc sillimanite knot retrograded to quartz and muscovite In granitic pegmatite. Note "feathery" habit of sillimanite (SIL) and close spatial association of quartz (QTZ) which Indicates In situ crystallization from melt. Synco Road In Pelletier Township.

Photo 75: Connected sillimanite aggregates (SIL) forming "ropes" In granitic pegmatite (FELO and QTZ). Preservation of sillimanite Indicates crystallization from peraluminous magma and minimum conditions of formation were 72S*C at Skbar. Photo was taken at same location as 7a. Field of view is *5 cm across. -75-

wag^*** Photo 8a: The occurrence of tourmaline (black mineral) characterizes the pegmatite zone adjacent to and intrusive into the supracrustal rocks. Holes in upper left hand corner mark positions of eroded garnet (GT). Part of pegmatite dike intruding basalts 100 m north of forest access road 25-8-14 in Pelletier Township.

Photo 8b: Close-up of portion of Photo 8a. Black tourmaline (TOUR) exhibits a graphic-like texture in quartz (QTZ) both surrounded by white weathering albite and microcline (FELD). This texture possibly originated by exsolution. -76-

Photo 9: Typical DI fold in metasediments showing quartz vein concentrations in fold closure. Note lineation(Li) is arked by plunge of small scale fold which is characteristic of DI folding. Photo from outcrop in northern Rykert Township.

Photo 10: Typical DZ interference fold pattern in metasediments showing northeast FZ axes. In western part of map

area similar fold patterns show northwest ?2 axcj - Photo taken from outcrop an CSR 10 east of Fergus Lake in Fergus Township. -77-

Photo 11 j Transposition of units (outlined in black) is a common 02 feature that prohibits development of a reliable stratigraphy and frequently localizes sulphide mineralization in the resultant shear zones. Photo from same location as Photo 10. -78-

Table 1; Table of Lithologic Units CENOZOIC QUATERNARY RECENT Swamp, lake, stream deposits PLEISTOCENE Glaciolacustrine, glaciofluvial deposits UNCONFORMITY PRECAMBRIAN PROTEROZOIC AND ARCHEAN MAFIC INTRUSIONS Diabase INTRUSIVE CONTACT LATE ARCHEAN Felsic Intrusions Granite, hornblende-biotite granodiorite, quartz monzonite, tonalite, granite pegmatite. Stray Lake Pluton biotite granodiorite INTRUSIVE CONTACT Migmatites-Gneiss Orthogneiss, paragneiss, metatexite, diatexite Metamorphic-Intrusive Contact Mafic and Intermediate Intrusions Gabbro, pyroxenite, biotite-pyroxene gabbro hornblende monzonite METAMORPHIC-INTRUSIVE CONTACT METAVOLCANICS AND METASEDIMENTS Metasediments Wacke, amphibolitic metasediments, chert, volcanogenic wacke, sulphide-oxide facies ironstones Felsic Metavolcanics and related Subvolcanic Intrusions Rhyolite and dacite flows, tuffs, pyroclastics, feldspar porphyry dikes, feldspar porphyry, quartz-feldspar porphyry, granodiorite, quartz-muscovite schist. Mafic to Intermediate metavolcanics Massive, foliated and pillowed flows, pillow breccias, ash and lapilli tuffs, pyroclastic breccias, debris flows, amphibolite, basaltic sills and dikes. -79-

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Hearst-Kapuskasing Area District of Cochrane Scaie 1:31 680 1 inch to 1/2 mile N.T.S. Reference: 42G2NW, 42G3N, 42G4NE, 42G5SE, 42G6S, 42G7SW ODM-GSC Aeromagnetic Maps: 2223G, 2224G, 2237G, 2238G, 2252G, 2251G ODM Geological Compilation Map: 2166 Please Note:

New use of Geographic Names 1) Stray Lake Pluton 2) Rufus Lake Fault -84-

Hearst-Kapuskasing Area LEGEND 1 ARCHEAN AND PROTEROZOIC DIABASE 7 Unsubdivided2 7a Dike, contains euhedral feldspar phenocrysts 7b Dike, feldspar phenocrysts absent, may or may not be magnetic INTRUSIVE CONTACT ARCHEAN FELSIC INTRUSIVE ROCKS 6 Unsubdivided2 6a Tonalite, trondhjemite, biotite-hornblende bearing 6b Quartz Monzonite, hornblende bearing 6c Granodiorite, biotite, biotite-hornblende bearing 6d Pegmatite, massive, white weathering 6e Peqmatite,Pegmatite, contains quartz * muscovite * sillimanite aggregates 6f Pegmatite, dikes INTRUSIVE CONTACT GNEISSIC ROCKS 5 Unsubdivided^ 5a Orthogneiss^ 5b Paragneiss3 5c Metatexite^ (less than or equal to 50% mobilizate) 5d Metatexite (greater than 50% mobilizate) 5e Diatexite 5 (less than or equal to 50% mobilizate) 5f Diatexite (greater than 50% mobilizate) Intrusive Metamorphic Contact MAFIC TO INTERMEDIATE INTRUSIVE ROCKS 4 Unsubdivided6 4-a Gabbro 4-b Pyroxenite, soft grey-green weathering 4c Monzonite, white to pink weathering, equigranular, hornblende bearing 4d Biotite-pyroxene gabbro, bright green weathering INTRUSIVE CONTACT METASEDIMENTARY ROCKS 3 Unsubdivided 2 3a Wacke, turbiditic, brown to grey weathering, biotite biotite-hornblende, biotite-muscovite bearing 3b Amphibolite, interflow units, dark green to black weathering 3c Chert, recrystallized 3d Volcanogenic wacke, reworked tuff 1F Sulphide-Oxide Facies Ironstones FELSIC METAVOLCANIC ROCKS 2a Flows; massive to foliated, white weathering 2b Tuff and lapilli tuff, lapillistone 2c Pyroclastic breccia, tuff breccia -85-

2d Feldspar Porphyry, commonly as brown to buff weathering dikes 2e Quartz-muscovite schist, commonly crenulated 2f Quartz-feldspar porphyry, feldspar porphyry, granodiorite, parts of subvolcanic pluton MAFIC TO INTERMEDIATE METAVOLCANIC ROCKS 1 Unsubdivided6 1a Flows, massive to foliated 1b Flows; pillowed 1c Pillow breccia 1d Tuff and lapilli tuff 1e Pyroclastic breccias, lapilli breccia, debris flows 1f Amphibolite, contains quartz-plagioclase-epidote knots, and stringers 1g Basaltic sills and dikes Notes i

1 Legend includes revisions based on laboratory investigations. 2 Outcrop from airphoto interpretation or aerial observation. This outcrop was not examined 3 Recognizable protolith preserving regional foliation observed in supracrustal rocks 4 Unrecognizable protolith but retains regional foliation observed in supracrustal rocks 5 Unrecognizable protolith with variable foliation in response to local stresses. 6 Rock type inferred from diamond drill logs, subdivision uncertain

Magnetic declination is 5o20©W (1985) in central part of map area D - Geology inferred from diamond drill logs, subdivision uncertain -86-

PROPERTIES AND OCCURRENCES 1 Campbell, R. [1960] Caithness Township 2 Kenogamisis, Gold Mines Limited [1965] Ecclestone Townships 3 Macassa Mines Limited [1960] Caithness Township 4- Vukmirovich, S. [1974, 1976, 1977, 1980] Caithness Township 5 Wabano, M. [1980] Caithness Township METAL AND MINERAL REFERENCE bio - Biotite mag - Magnetite carb- Carbonate mo Molybdenite cp - Chalcopyrite po - Pyrrhotite gf - Graphite py - Pyrite gt - Garnet qv - Quartz vein K-spar Alkali Feldspar tour- Tourmaline vns - Veins -87-

SOURCES OF INFORMATION Geology by B.R. Berger, D.W. MacMillan, P.L. Roy and assistants, 1985. Base maps compiled from Forest Resources Inventory maps, Division of Lands, Ministry of Natural Resources Geology is not tied to survey lines Records of assessment work on file at Resident Geologist©s Office, Timmins and Assessment Files Research Office (AFRO), Ontario Bennett, G., Brown, D.D., George, P.T., Leahy, T., 1967, Operation Kapuskasing: Ontario Department of Mines, Miscellaneous Paper 10, 98 p. Accompanied by maps P. 397 and P. 398, scale 1:127,520 or 1 inch to 2 miles -88-

List of Maps Bourinot - Ecclestone 492 831 Opazatika - Fergus 492 832 Abbott - Rykert 492 833 Pelletier - Doherty 493 824 Cargill - Ecclestone 493 831 Fergus - Ecclestone 493 832 Rykert - Caithness 493 833 Caithness - Scholfield PROVINCE OF ONTARIO 83 30 DEPARTMENT OF LANDS AND FORESTS FOREST RESOURCES INVENTORY 83 15

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