Kimberlite, Base Metal and Gold Exploration Targets, Opasatika

Ontario Geological Survey Open File Report 5982

Kimberlite, Base Metal and Gold Exploration Targets Based upon Heavy Mineral Data Derived from Surface Materials, Opasatika Lake Area, Northeastern Ontario

1999

ONTARIO GEOLOGICAL SURVEY

Open File Report 5982

Kimberlite, Base Metal and Gold Exploration Targets Based upon Heavy Mineral Data Derived from Surface Materials, Opasatika Lake Area, Northeastern Ontario

D.M Stephenson, T.F. Morris and D.C. Crabtree

1999

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: Stephenson, D.M., Morris, T.F. and Crabtree, D.C. 1999. Kimberlite, base metal and gold exploration targets based upon heavy mineral data derived from surface materials, Opasatika Lake area, northeastern Ontario; Ontario Geological Survey, Open File Report 5982, 59p.

e Queen’s Printer for Ontario, 1999 e Queen’s Printer for Ontario, 1999. Open File Reports of the Ontario Geological Survey are available for viewing at the Mines Library in Sudbury, at the Mines and Minerals Information Centre in Toronto, and at the regional Mines and Minerals office whose district includes the area covered by the report (see below). Copies can be purchased at Publication Sales and the office whose district includes the area covered by the report. Al- though a particular report may not be in stock at locations other than the Publication Sales office in Sudbury, they can generally be obtained within 3 working days. All telephone, fax, mail and e--mail orders should be directed to the Publi- cation Sales office in Sudbury. Use of VISA or MasterCard ensures the fastest possible service. Cheques or money orders should be made payable to the Minister of Finance. Mines and Minerals Information Centre (MMIC) Tel: (416) 314-3800 Macdonald Block, Room M2-17 1--800--665--4480(toll free inside Ontario) 900 Bay St. Toronto, Ontario M7A 1C3 Mines Library Tel: (705) 670-5615 933 Ramsey Lake Road, Level A3 Sudbury, Ontario P3E 6B5 Publication Sales Tel: (705) 670-5691(local) 933 Ramsey Lake Rd., Level A3 1-888-415-9847(toll-free) Sudbury, Ontario P3E 6B5 Fax: (705) 670-5770 E-mail: [email protected]

Regional Mines and Minerals Offices: Kenora - Box 5050, 810 Robertson St., Kenora P9N 3X9 Kirkland Lake - 10 Government Rd. E., Kirkland Lake P2N 1A8 Red Lake - Box 324, Ontario Government Building, Red Lake P0V 2M0 Sault Ste. Marie - 70 Foster Dr., Ste. 200, Sault Ste. Marie P6A 6V8 Sioux Lookout - Box 3000, Queen and Fourth, Sioux Lookout P8T 1C6 Southern Ontario - P.O. Bag Service 43, Old Troy Rd., Tweed K0K 3J0 Sudbury - Level B3, 933 Ramsey Lake Rd., Sudbury P3E 6B5 Thunder Bay - Suite B002, 435 James St. S., Thunder Bay P7E 6S7 Timmins - Ontario Government Complex, P.O. Bag 3060, Hwy. 101 East, South Porcupine P0N 1H0 Toronto - MMIC, Macdonald Block, Room M2--17, 900 Bay St., Toronto M7A 1C3

This report has not received a technical edit. Discrepancies may occur for which the Ontario Ministry of Northern Devel- opment and Mines does not assume any liability. Source referencesare included in the report and users are urged to verify critical information. Recommendations and statements of opinions expressed are those of the author or authors and are not to be construed as statements of government policy. If you wish to reproduce any of the text, tables or illustrations in this report, please write for permission to the Team Leader, Publication Services, Ministry of Northern Development and Mines, 933 Ramsey Lake Road, Level B4, Sudbury, Ontario P3E 6B5.

Cette publication est disponible en anglais seulement. Parts of this report may be quoted if credit is given. It is recommended that reference be made in the following form:

Stephenson, D.M., Morris, T.F. and Crabtree, D.C. 1999. Kimberlite, base metal and gold exploration targets based upon heavy mineral data derived from surface materials, Opasatika Lake area, northeastern Ontario; Ontario Geological Survey, Open File Report 5982, 59p.

iii

Contents

Abstract ...... xi Introduction ...... 1 Project History and Purpose ...... 1 Study Location ...... 4 Physiography ...... 4 Regional Geology ...... 4 Bedrock Geology ...... 4 Quaternary Geology ...... 6 Methods ...... 6 Material Sampling ...... 6 Pebble Lithology ...... 7 Heavy Mineral Recovery and Identification...... 7 Kimberlite Indicator Minerals ...... 8 Garnet ...... 8 Chromite ...... 8 Mg-ilmenite ...... 8 Cr-diopside ...... 8 Metamorphosed Magmatic/Massive Sulphide Indicator Minerals...... 9 Cr-diopside ...... 9 Chromite ...... 9 Gahnite ...... 9 Data Plotting Parameters ...... 9 Results ...... 10 Pebbles ...... 10 Kimberlite Indicator Minerals ...... 11 Cr-pyrope Garnet ...... 11 Chromite ...... 11 Mg-ilmenite ...... 15 Cr-diopside ...... 25 Recommendations for Kimberlite Exploration...... 25 Metamorphosed Magmatic/Massive Sulphide Indicator Minerals...... 34 Gahnite ...... 34 Ruby Corundum ...... 34 Olivine ...... 40 Recommendations for Metamorphosed Magmatic/Massive Sulphide Exploration...... 40 Gold Grains ...... 45 Acknowledgements ...... 49 References ...... 50 Appendix 1: Sample Site Locations...... 53 Appendix 2: Sample Normalization Calculations...... 57 Metric Conversion Table ...... 59 Tables 1. Summary of the number of chromite grains based on normalization of the data...... 10 2. Comparison of local vs. exotic pebbles in different sampling media...... 11 3. Summary of statistics for KIMs ...... 15

4. Summary of reduced vs. oxidized environments for Mg-ilmenite grains...... 24 5. Recommended areas for kimberlite exploration based on total KIMs...... 32 6. Recommended areas for kimberlite exploration based on normalized data for total KIMs...... 33 7. Summary of statistics for MMSIMs...... 35 8. Recommended areas for massive sulphide exploration based on total MMSIMs...... 43 9. Recommended areas for massive sulphide exploration based on normalized data for total MMSIMs...... 44 10. Summary of statistics for gold grains...... 45 11. Recommended areas for gold exploration based on raw data for total gold grains...... 48 12. Recommended areas for gold exploration based on normalized data for total gold grains...... 49

Figures 1. Locations of the 1997 and 1998 overburden mapping and sampling programs...... 2 2. Study area location, 1998 ...... 3 3. Bedrock geology ...... 5 4. Pebble lithology of modern alluvium sample 108-MA-98...... 12 5. Pebble lithology of modern alluvium sample 30-MA-98...... 12 6. Regional distribution of exotic clasts in pebble counts...... 13

7. “G10” and “G9” Cr-pyrope garnet Cr2O3 - CaO plot...... 14 8. Regional distribution of Cr-pyrope garnet grains based on raw data...... 16 9. Regional distribution of Cr-pyrope garnet grains based on normalized data...... 17

10. Eclogitic garnet TiO2 -Na2Oplot...... 18

11. Chromite Cr2O3 - MgO plot ...... 19

12. Chromite Cr2O3 -TiO2 plot ...... 20 13. Regional distribution of chromite grains...... 21 14. Regional distribution of chromite grains based on normalized data...... 22

15. Mg-ilmenite Cr2O3 - MgO plot ...... 23 16. Regional distribution of Mg-ilmenite grains based on raw data...... 26 17. Regional distribution of Mg-ilmenite grains based on normalized data...... 27 18. Regional distribution of Cr-diopside grains...... 28 19. Regional distribution of Cr-diopside grains based on normalized data...... 29 20. Regional distribution of total KIMs...... 30 21. Regional distribution of total KIMs based on normalized data...... 31 22. Regional distribution of gahnite grains based on raw data...... 36 23. Regional distribution of gahnite grains based on normalized data...... 37 24.GahniteMgO-ZnO-FeOplot...... 38 25. Regional distribution of Group 1 vs. Group 2 gahnite grains...... 39 26. Regional distribution of total MMSIMs...... 41 27. Regional distribution of total MMSIMs based on normalized data...... 42 28. Regional distribution of total gold grains based on raw data...... 46 29. Regional distribution of total gold grains based on normalized data...... 47

vii

*Miscellaneous ReleaseZData 41 Kimberlite, base metal and gold exploration targets based upon heavy mineral data derived from surface materials, Opasatika Lake area, northeastern Ontario; by D.M. Stephenson. This release consists of data related to kimberlite indicator minerals, metamorphosed magmatic/massive sulphide indicator minerals and gold grains recovered from modern alluvium, till and glaciolacustrine samples collected in the Opasatika Lake area, southwest of Kapuskasing, northeastern Ontario. This data release consists of 12 data files stored as both tab delimited, ASCII (.txt) and Microsoft Excel (.xls) files. Data sets consist of: 1) definitions of abbreviations used in each of the data files (Intro); 2) sample site locations (AppA); 3) pebble data summary (AppB); 4) sample processing data (AppC); 5) detailed gold grain summary (AppD); 6) summary of kimberlite indicator minerals counts (AppE); 7) summary of metamorphosed magmatic/massive sulphide indicator mineral counts (AppF); 8) summary of microprobe data for KIMs (AppG); 9) summary of microprobe data for metamorphosed magmatic/ massive sulphide indicator minerals (AppH); 10) summary of microprobe data for non-kimberlite indicator minerals (AppI); 11) heavy mineral picking remarks (AppJ); 12) summary of secondary metamorphosed magmatic/massive sulphide indicator mineral counts (AppK). These files are on one 3.5 inch MS-DOS diskette in a self-extracting, compressed format. Extracting instructions are included.

This diskette is available separately from the report.

Abstract This report provides data and preliminary interpretations on the types and distribution of kimberlite heavy mineral indicators, metamorphosed magmatic/massive sulphide indicator minerals and gold grains recovered from modern alluvium, till and glaciolacustrine samples collected in the Opasatika Lake area, south of Kapuskasing, Ontario. This data can be used to focus exploration efforts for kimberlite, base metal and gold deposits. A total of 123 modern alluvium, 25 till and 11 coarse-grained glaciolacustrine samples were collected from across the area. From these samples, 3 “G10” Cr-pyrope garnets were recovered as well as one high-Na eclogitic garnet. The recovery of these grains is significant, as they are rare and commonly associated with diamond- bearing kimberlite. Five areas and 4 individual sites were identified as potential sites for further kimberlite exploration. A number of metamorphosed magmatic/massive sulphide indicator minerals were recovered including 9 gahnite grains. Gahnite is also rare and is considered an excellent indicator of potential metamorphosed magmatic/massive sulphide mineralization. Based on the data, 3 areas and 3 individual sites are recommended for further base metal exploration. Very few gold grains were recovered from the samples, however, one pristine gold grain was recovered indicating relatively close proximity to source. Three areas and 6 individual sites were identified as having gold concentrations above background levels.

Introduction PROJECT HISTORY AND PURPOSE Kimberlite is recognised as the primary host rock for diamond. A suite of heavy minerals (Cr-pyrope garnet, chromite, Mg-rich ilmenite, Cr-diopside and olivine) is commonly associated with kimberlite and are referred to as kimberlite indicator minerals (KIMs). Quaternary geology mapping and modern alluvium sampling programs conducted by the Ontario Geological Survey (OGS) in the Wawa area, northeastern On- tario, were successful in defining the presence of KIMs, their distribution and relative abundance (Morris 1990, 1991, 1992a, 1992b, 1994a, 1994b, 1995a, 1995b, 1996a, 1997a, 1997b, 1998; Morris et al. 1994; Morris et al. 1997; Morris et al. 1998). This work also established a link between the distribution of KIMs and regional faults associated with the Kapuskasing Structural Zone (KSZ). The KSZ is a broad belt of high grade metamorphic rock thought suitable for hosting kimberlite (Boland and Ellis 1989). The KSZ and associated faults extend northeast from Wawa through the Kapuskasing area into the James Bay Low- land (Figure 1). Given the success of the Wawa project a need existed to determine whether other areas along the KSZ were suitable for kimberlite exploration. To meet this need, the OGS initiated an overburden mapping and sampling program south of Kapuskasing. During the summer of 1997, Quaternary geology mapping and a modern alluvium sampling program were completed in the Woman Falls-Wakusimi River area (Figure 1). As part of a Quaternary geology mapping and overburden sampling program in the Separation Lake area, northwestern Ontario (Morris 1996b) and the Woman Falls-Wakusimi River area (Morris 1998), till samples were analyzed for metamorphosed magmatic/massive sulphide indicator minerals (MMSIMsR)*. These are stable minerals associated with metamorphosed magmatic or massive sulphide deposits hosted in high-grade metamorphic terranes. Many sulphide minerals are quickly destroyed by weathering when dis- persed into the near surface environment. As a result, sulphide deposits are difficult to detect by conven- tional geochemical exploration methods. High-grade metamorphism, however, produces a suite of indicator mineral species, which are heavy, visually distinctive, chemically stable and usually coarse-grained. These heavy minerals include: aluminum, magnesium, manganese, and chromium silicates such as sillimanite, staurolite, sapphirine, anthophyllite, hypersthene, olivine, spessartine, red epidote, and chromium-diopside; and chrome, zinc or titanium oxides such as chromite, ruby corundum, gahnite and red rutile. In addition to metamorphosed magmatic/massive sulphide deposits, gahnite is also used as an indicator of rare element pegmatites (Morris et al. in press). The Woman Falls-Wakusimi River project was successful in establishing the occurrence of KIMs, MMSIMs and gold grains (Morris 1997a, 1998; Morris, Crabtree, and Averill 1998). The relative proximity to source of indicator minerals was determined through evaluation of the pebble component of samples and limited geophysical data. A relationship between the occurrence of KIMs and bedrock structure was also established. From this work, several excellent exploration targets for kimberlite, base metals and gold were identified. In the summer of 1998, modern alluvium sampling and overburden mapping was extended west to the Opasatika Lake-Roche Lake area (Figure 2). This study provides a general assessment of the potential for kimberlite exploration along the western flank of the KSZ and a specific assessment of the potential for kimberlite, base metals and gold for the Opasatika Lake-Roche Lake area. The program has several objectives: 1) to enhance the regional data base on the types, distribution and relative abundance of KIMs, MMSIMs and gold grains found in modern alluvium, till and coarse-grained glaciolacustrine sediments; 2) to determine if the occurrence of KIMs and their relationship to bedrock structure continues west across the KSZ; and 3) to extend surficial geology mapping west in order to pro- vide a framework for interpreting heavy mineral and geochemical anomalies and for use in environmental and land-use planning exercises. Modern alluvium was the principal material sampled. A few coarse-grained glaciolacustrine samples were collected for background reference. In addition, a limited number of till samples were collected to establish glacial dispersal characteristics from a mafic-ultramafic pluton.

* MMSIM is a registered trademark of Overburden Drilling Management Limited, Nepean, Ontario

1 2 3 This report summarizes the types, concentrations and distribution of KIMs, MMSIMs and gold grains recovered from the different surficial materials. Recommendations for kimberlite, base metal and gold exploration are proposed. The data is summarized in digital format (Stephenson 1999); data consists of the following ASCII (.txt) and Microsoft Excel (.xls) files: 1) Intro: Definitions of abbreviations; 2) AppA: Sample site locations; 3) AppB: Pebble data summary; 4) AppC: Sample processing data; 5) AppD: Detailed gold grain summary; 6) AppE: Summary of kimberlite indicator minerals counts; 7) AppF: Summary of metamorphosed magmatic/massive sulphide indicator mineral counts; 8) AppG: Summary of microprobe data for KIMs; 9) AppH: Summary of microprobe data for metamorphosed magmatic/massive sulphide indicator minerals; 10) AppI: Summary of microprobe data for non-kimberlite indicator minerals; 11) AppJ: Heavy mineral picking remarks; 12) AppK: Summary of secondary metamorphosed magmatic/massive sulphide indicator mineral counts;

STUDY LOCATION The Opasatika Lake-Roche Lake study area is located immediately west of the Woman Falls-Wakusimi River area study (Morris et al. 1998). The Woman Falls-Wakusimi River area was originally chosen due to the presence in this area of several fault controlled structures related to the KSZ, relatively thin overburden cover and easy access from Kapuskasing. The Opasatika Lake-Roche Lake area is represented on 2, 1:50 000 scale National Topographic Series maps. The western part of the study area is covered by the Roche Lake (42 G/4) sheet and the eastern part by the Opasatika Lake (42 G/3) sheet. The area is bounded by longitudes 84L00i W and 83L00i W and lati- tudes 49L00i N and 49L15i N.

PHYSIOGRAPHY The study area is located north of the Great Lakes-Hudson Bay drainage divide. All surface drainage flows north into James Bay. There are 4 major drainage basins within the study area. These include the Matta- witchewan, Goat, Missinaibi and Opasatika rivers. The Opasatika Lake-Roche Lake area is part of the Abitibi Uplands subregion of the James physiographic region (Bostock 1976). Much of this subregion is underlain by crystalline Archean rocks and has a broad rolling surface that rises gently from the Hudson Bay Lowland. Much of the topography in the Opasatika Lake area is subtle; local relief is up to 45 m. In the Roche Lake area, the topography is more pronounced with local relief of up to 120 m. Bedrock outcrops occur most commonly in the Roche Lake area and along parts of the Missinaibi and Brunswick rivers in the Op- asatika Lake area.

Regional Geology

BEDROCK GEOLOGY The bedrock geology of the area consists of 7 Archean-age bedrock types (Berger 1986; Ontario Geological Survey 1991; Figure 3). These include: 1) muscovite-bearing granitic rocks including muscovite-biotite and cordierite-biotite granites, granodiorite to tonalite; 2) a foliated tonalite suite consisting of tonalite to granodiorite, foliated to massive; 3) a gneissic tonalite suite consisting of tonalite to granodiorite, foliated to gneissic, with minor supracrustal inclusions; 4) mafic and ultramafic rocks including gabbro and anortho-

4 5 site; 5) metasedimentary rocks including wacke, arkose, argillite, slate, marble, chert, iron formation, and minor metavolcanic rocks; 6) felsic to intermediate metavolcanic rocks including rhyolitic, rhyodacitic, dacitic and andesitic flows, tuffs and breccias, chert, iron formation, minor metasedimentary and intrusive rocks and related migmatites; and 7) mafic to intermediate metavolcanic rocks including basaltic and andesitic flows, tuffs and breccias, chert, iron formation, minor metasedimentary and intrusive rocks and related migmatites. All of the above units are cut by northwest trending Proterozoic diabase dikes of the Matache- wan and Hearst swarms. Northeast trending Proterozoic diabase dikes of the Preissac swarm outcrop in the southeastern part of the field area and northeast trending Proterozoic diabase dikes of the Abitibi swarm cut across units in the western part of the field area. The Rufus Lake Fault strikes northeast across the eastern part of the map area. A second set of faults striking northwest and northeast occur in the Brunswick Lake area. Many of the lake and stream orienta- tions are perpendicular to the KSZ structural trend and appear to be structurally controlled. The KSZ is significant as it consists of fractured, deep crustal material that may host kimberlite rock (Boland and Ellis 1989).

QUATERNARY GEOLOGY All glacial landforms and materials in the map area were likely formed and deposited during the Wisconsin glaciation. Striae, groove and drumlinoid features define ice flow direction. Three sets of striae were observed: 110L-162L, 170L-195L, and 200L-260L Crosscutting striae relationships on 2 outcrops clearly dem- onstrate that striae oriented southeast (110L-162L) are the youngest. In the eastern part of the study area, one outcrop surface consisted of striae oriented 135L that cross-cut striae oriented 170L-195L. On a second outcrop, in the central part of the map area, striae orientated 144L crosscut striae oriented at 210L.The 110L-162 L set of striae is the most prevalent and was observed on numerous outcrops throughout the area. The relative age relationship between the 170L-195L and 200L-260L flow events is not clear. Similar striae observations were made to the east in the 1997 survey (Morris 1997a). Observations on the types and distribution of surficial materials were made at each sample site. These observations were integrated with aerial photo interpretation to establish the types and distribution of overburden materials and related landforms associated with glacial and post-glacial events in the area. In turn, these observations will be combined with those from the 1997 work to produce a composite overburden map and accompanying Quaternary geology report. Methods

MATERIAL SAMPLING In this study, modern alluvium, till and glaciolacustrine materials were sampled. In total, 123 modern alluvium, 25 till and 11 coarse-grained glaciolacustrine samples were collected. Sample numbers, sample types and locations (by UTM coordinates) are summarized in Appendix 1 and in Stephenson (1999, Ap- pendix A). Modern alluvium was chosen as the primary sampling media as it is commonly used as a means of gaining a fast, relatively inexpensive heavy mineral signature for individual drainage basins. The heavy mineral signature obtained from modern alluvium is a product of the erosion of both bedrock and overburden, and the subsequent transportation and deposition of the eroded material. A more detailed discussion of the controls of these processes can be found in Morris et al. (1994), Morris (1995b), and Morris and Kas- zycki (1997). It is important to note, however, that lakes within drainage basins act as sediment traps, re- stricting the down drainage transport of heavy minerals. Therefore, when modern alluvium sample sites were chosen for this study, an attempt was made to maximize the length of stream section between the sample site and a lake. This maximizes the area of drainage basin sampled by the stream. To maintain continuity with the data collected in 1994 (Morris et al.1994), 1996 (Morris et al. 1997, Morris et al. 1998) and 1997 (Morris, Crabtree and Averill. 1998), the same sampling procedure employed in those programs was used in this sampling program. Modern alluvium was collected from bars or sediment traps within streams where heavy minerals are concentrated. Material was sifted through a 7 mm mesh, steel sieve to exclude the coarse fraction. A minimum of 10 kg of less than the 7 mm sized material

6 was collected at each site. At sites where the material was fine-grained, a minimum of 15 kg of less than 7 mm sized material was collected to ensure a sufficient amount of concentrate was obtained. A sample of the greater than 7 mm sized fraction was collected for determination of pebble lithology (Stephenson 1999, Appendix B). Modern alluvium was also panned at each site and the concentrate was stored for future reference. Coarse-grained glaciolacustrine and ice-contact stratified drift materials were sampled from all accessi- ble sand and gravel pits. Material was sifted through a 7 mm mesh, steel sieve to exclude the coarse fraction. A minimum of 10 kg of less than 7 mm sized material was collected at each site. A sample of the greater than 7 mm sized fraction was collected for determination of pebble lithology (Stephenson 1999, Appendix B). Till sampling was completed in an area underlain by a mafic-ultramafic pluton. Till samples were collected up-ice, over and down-ice of this pluton to establish glacial dispersal characteristics for the area. Due to the fine-grained nature of the till, field sieving was not necessary. At each site, 2 samples of the till “C” horizon were taken. A 200 g sample was submitted for instrumental neutron activation analysis (INAA), and inductively coupled plasma-mass spectrometry (ICP-MS) and inductively coupled plasma-atomic emission spectrometry (ICP-AES) geochemical analysis. This data will be released at a later date. A 15 kg sample was submitted for heavy mineral concentration and subsequent analysis. A pebble sample was also taken at each site for determination of pebble lithology. Observations made at each sample site included both a site description (sample site material type; surrounding material type; presence of bedrock or boulders; topography; channel/surface slope; stream flow; drainage of surrounding area; and vegetation) and a material description (texture; abundance, size, shape, surface features and types of clasts; and bar form). A more detailed explanation of the types of observations made are reported in Morris and Kaszycki (1997).

PEBBLE LITHOLOGY Pebble lithology was determined by comparing the physical properties of pebbles to representative samples of local bedrock. Pebble lithologies identified include: granite; gneiss; metasediment; mafic metavolcanic; felsic metavolcanic; ultramafic phaneritic, carbonate; quartz; and sandstone.

HEAVY MINERAL RECOVERY AND IDENTIFICATION All samples were sent to Overburden Drilling Management Ltd. in Nepean, Ontario for processing to iso- late gold grains, KIMs and MMSIMs. This procedure is discussed in detail elsewhere and will not be re- peated here (Morris and Kaszycki 1997). Excepting gold, once the indicator grains were picked from the samples, microprobe analysis was completed to determine grain composition. Sample processing data, including weight of table feed and weight of both non-magnetic and magnetic fractions, are summarized in Stephenson (1999, Appendix C). A detailed gold grain summary is provided in Stephenson (1999, Appendix D). The physical appear- ance of each gold grain was evaluated and classified as being pristine, modified or reshaped. Due to the gold’s malleability, grain shape is transformed during transport by glacial ice (DiLabio 1990). Therefore, a reshaped grain is more likely to have been transported farther from source than a pristine one. During processing, 6 types of KIMs are recovered: Cr-pyrope garnet; Cr-poor megacrystic pyrope garnet; eclogitic pyrope-almandine garnet; Cr-diopside; Mg-rich ilmenite; and chromite. Forsteritic olivine, a mineral commonly associated with kimberlite, was also picked when observed in the heavy mineral concentrate (Stephenson 1999, Appendix E). Processing also recovered 13 main types of MMSIMs: anthophyllite; chalcopyrite; chromite; Cr-diopside; gahnite; hypersthene; olivine; ruby corundum; red epidote; red rutile; sapphirine; spessartine and staurolite (Stephenson 1999, Appendix F). Other MMSIM species are also reported where present (Stephenson 1999, Appendix K). Potential KIM grains were mounted on epoxy plugs and sent to the Ontario Geosciences Centre (OGC) for microprobe analysis in order to determine precise grain composition (Stephenson 1999, Appendix G).

7 From the MMSIMs only gahnite, ruby corundum and olivine compositions were determined by microprobe analysis (Stephenson 1999, Appendix H). The calibration routine and operating conditions for the microprobe are summarized in Morris et al. (1994) and Morris et al. (1997). Prior to mounting for microprobe analysis, the grains were photographed with a stereomicroscope using 64 ASA tungsten slide film.

KIMBERLITE INDICATOR MINERALS Garnet Garnet grains analyzed in this study include Cr-pyrope, pyrope, almandine, andradite and spessartine. Gar- nets of peridotite origin are typically Cr-rich pyropes. This mineral may originate from many different types of peridotite, but the most important are harzburgite and lherzolite. Eighty-five percent of Cr-pyrope that occur as inclusions in diamonds are Ca-depleted, Cr-enriched and harzburgitic in origin (Gurney 1984). These types of garnet have been termed “G10” (Dawson and Stephens 1975). The recovery of “G10” garnets from surficial material is important since it suggests that these minerals originated from harzburgitic peridotite and are more strongly associated with diamonds than are garnets of lherzolitic (“G9”) origin (Dawson and Stephens 1975). Other pyrope garnets associated with kimberlites are the megacrystic suite, which are not directly associated with diamond. These, when found with other KIMs, can also be useful indicators. These minerals may range from Cr-poor to moderate levels (2 to 3 wt %) of Cr2O3. The composition of mantle derived eclogitic garnet is complex and overlap may exist between garnets of peridotitic and deep crustal origin (Dawson and Stephens 1975). However, eclogitic garnets are typically Cr-poor and range from pyrope to almandine-pyrope in composition. Eclogitic garnet inclusions in diamond have been found to have elevated sodium concentrations (Na2O greater than 0.07%) (Fipke et al. 1995) and, like the “G10” garnet, are considered a valuable KIM. Low-Na eclogitic garnets may also be useful indicators if found in conjunction with other KIMs. Almandine, spessartine-almandine, grossular and andradite garnets are not likely associated with kimberlite and are, therefore, of little interest to kimberlite exploration. Chromite

Chromites found in diamond inclusions differ from most other chromites by their high Cr2O3 content, generally greater than 61 wt % (Gurney 1984). In addition, they also have an MgO content greater than 10 wt % (Fipke et al.1995). These chromites are termed “inclusion field” chromites since they plot in the diamond inclusion field on a chromite Cr2O3-MgO plot. Finding such a chromite in surficial material or a rock sample is just as significant as finding a “G10” Cr-pyrope garnet.

Chromite Cr2O3-TiO2 plots are useful in differentiating chromite unique to lamproites and kimberlites from those that are non-lamproitic or non-kimberlitic in origin (Fipke et al. 1995). Those chromites that plotted in the non-lamproite/kimberlite field were excluded from the KIM database (Stephenson 1999, Ap- pendix I). Those that plotted in the overlap field and the field unique to kimberlites and lamproites were included in the KIM database (Stephenson 1999, Appendix G). Mg-ilmenite Ilmenite found within kimberlite is generally Mg-rich with MgO values that range between 4 and 15 wt % (McCallum and Vos 1993). In this study, such ilmenites recovered from overburden are regarded as useful KIM indicators (Stephenson 1999, Appendix G). A Mg-ilmenite parabolic plot (Cr2O3 versus MgO) (Gurney and Moore 1991) can be used to determine if the ilmenite grains originated from a reducing environment (favourable for diamond preservation within the magma) or from an oxidizing environment (con- ducive to diamond resorption into the magma). Cr-diopside Cr-diopside is not a definitive kimberlite indicator since it occurs in both kimberlite and other basic and ultrabasic rocks. Cr-diopside associated with lherzolitic rock commonly has high chrome values (greater

8 than 1 wt %). For this reason, Cr-diopsides with Cr2O3 values greater than 1 wt % were chosen as KIMs for this study (Stephenson 1999, Appendix G).

METAMORPHOSED MAGMATIC/MASSIVE SULPHIDE INDICATOR MINERALS Cr-diopside

In this study, Cr-diopsides with Cr2O3 values less than 1 wt % were chosen as MMSIMs (Stephenson 1999, Appendix H). Such Cr-diopsides are associated with nickel deposits in Finland (Stu Averill, Overburden Drilling Management Ltd., personal communication 1998) and with the Thompson nickel belt in Manitoba (Matile and Thorliefson 1997). Chromite Those chromites that plot in the non-lamproitic/kimberlitic field and overlap field of the Fipke et al. (1995) Cr2O3-TiO2 diagram were included in the MMSIM database (Stephenson 1999, Appendix H). Gahnite Gahnite is a useful indicator mineral in the search for polymetallic deposits in high grade metamorphic terrane due to its hardness (8) and stability in metamorphic rocks (Parr 1992). Although rare, gahnite is reported in a number of polymetallic deposits (Chew 1977; Plimer 1977; Spry 1982, 1987a, 1987b; Williams 1983; Sheridan and Raymond 1984; and Spry and Scott 1986). Gahnite was also successfully evaluated as an indicator mineral in glacial dispersal plumes from the Montauban polymetallic deposit in Quebec (La- londe et al. 1994). Gahnite is not only an indicator of polymetallic deposits within high grade metamorphic terranes but also of pegmatite (Cerny et al. 1981; Cerny and Hawthorne 1982). Little work has been done using mineral composition to differentiate gahnite found within different source rocks (Batchelor and Kinnaird 1984). Preliminary analysis of data from gahnite composition from known source rocks, as derived from the literature and analytical work carried out in conjunction with the Separation Lake, Kinniwabi Lake and Kapuskasing projects (Morris 1996b, 1997b, 1998; Morris et al. in press), indicate that gahnite from polymetallic deposits commonly has MgO values greater than 2 wt %. Gahnite from rare-element pegmatite has MgO values commonly less than 2 wt % (Morris 1998). Gahnite recovered from samples in this study were similarly classified. Data Plotting Parameters To identify areas or sites favourable for kimberlite, base metal or gold exploration, it is important to identify the location of important KIMs (“G10” Cr-pyrope garnet, “inclusion field” chromite), MMSIMs (gahnite, low Cr-diopside) and gold grains (pristine) and their relative abundance. The proportional dot diagrams presented in this report illustrate the relative abundance of heavy indicator minerals and their locations throughout the study area. These diagrams are based on statistics that involve calculating percentiles. The largest dots on the diagram represent sites with heavy mineral concentrations with values greater than the 95th percentile. Sites with these values are considered anomalous and are significant. The proportional dot diagrams in this report are presented in two different ways: 1) based on “raw data”; and 2) based on “normalized data”. In order for data to be compared between sample sites and compared with data collected in conjunction with the Wawa, Kinniwabi Lake and Kapuskasing projects (Morris 1994b, 1997, 1998), databases for the KIMs and MMSIMs have been normalized 2 ways. First, for reasons of practicality, estimates rather than precise counts of the number of heavy mineral indicators in some concentrates were inferred by the external lab (Stephenson 1999, Appendix J). For example, the heavy mineral concentrate of sample 76-MA-98 contained an estimated 15 chromites, however, only 4 chromite grains were picked. The composition of the 4 picked grains was used to determine the number of kimberlitic versus non-kimberlitic chromite grains present in the estimated population of 15 chromite

9 grains. Secondly, the data for KIMs, MMSIMs and gold grains were normalized by table feed weight against 15 kg. Sample calculations for both methods of normalization are presented in Appendix 2. For this report, “raw data” refers to the actual number of grains picked for each sample. However, in the case where grains counts were estimated within a concentrate, the raw data was normalized by count estimates as previously described. This was only required for samples involving chromite. This was necessary as a sample with an anomalous chromite number would not stand out as anomalous if the number of picked grains from that sample was the same as the background values derived from all the sample sites (Table 1). Separate normalization calculations were required for 2 Cr-diopside samples (10-MA-98 and 117-MA-98). In both cases, 2 Cr-diopside grains were picked, one was lost in the preparation of the plugs and the other was identified by microprobe analysis as being a high-chrome Cr-diopside. It was then as- sumed that the lost grain was a high-chrome Cr-diopside. Therefore, for both samples, the number of KIM Cr-diopsides recovered was reported as 2. The “normalized data” was normalized by both count estimates and table feed weight. Table 1: Summary of the number of chromite grains based on normalization of the data.

Sample No. of picked No. of estimated No. of grains identified by Normalized grain counts Number grains grains microprobe analysis KIM MMSIM KIM MMSIM 76-MA-98 4 15 2 2 8 8 85-GL-98 2 10 2 2 10 10 104-MA-98 7 15 6 7 13 15 106-MA-98 3 10 2 2 7 7 114-MA-98 6 15 5 5 13 13 116-MA-98 13 30 11 11 25 25

Results

PEBBLES Determining pebble lithology was difficult due to the complex composition of some rock domains. For example, the metasedimentary terrane consists of many rock types, some of which are not metasediments. Therefore, the composition of a pebble sample collected over, or down ice from such a terrane may reflect many different bedrock types, as opposed to just “metasedimentary” pebbles. Similarly, a pebble sample collected over a gneissic terrane may consist primarily of metavolcanics derived from a local inlier in the gneisses rather than from a more distal metavolcanic (Figure 4). Also, pebbles collected were generally 0.5 to 3 cm. Coarse gneissic banding may not be recognized in pebbles this size but rather a pebble from a felsic band may be interpreted as granitic in origin. Therefore, the percentages of gneissic pebbles may have been underestimated. Alternatively, there are certain pebbles that are not derived from local sources and their presence within a sample may be used as an indicator of the degree of distal material within that sample. For example, the presence of a large percentage of carbonate or sandstone clasts may indicate that much of that sample was derived from distal, not local, sources (Figure 5). In general terms, pebble lithology data derived from the modern alluvium, glaciolacustrine and till samples yielded similar averages and indicates a high percentage of pebbles derived from distal sources (Table 2) (Figure 6). Given the significant percentage of distally derived pebbles within each sample type, it is important to consider the pebble lithology of each sample individually. This will help evaluate the proximity of a heavy mineral signature to its source.

10 Table 2. Comparison of local (gneiss, granite, quartz and metavolcanic, metasedimentary) vs. exotic (carbonate and sandstone) pebbles in different sampling media.

Sample Type Total PebbleType(%) Samples Gn/Gr/Qu Mv/Ms Total Local Pebble Car/Ss

Modern 74 35 25 60 40 Alluvium

Glaciolacustrine 11 37 19 56 44

Till 25 28 35 63 37

Pebble Type Gn/Gr/Qu: Gneiss/Granite/Quartz Mv/Ms: Metavolcanic/Metasedimentary Car/Ss: Carbonate/Sandstone

KIMBERLITE INDICATOR MINERALS Cr-pyrope Garnet Of the 118 garnets submitted to the OGC for microprobe analysis, 3 were determined to be “G10” Cr-pyrope garnets and 35 were identified as “G9” Cr-pyrope garnets (Figure 7). Four grains were identified as eclogitic garnets. Other garnets identified include almandine, andradite, Ti-andradite and spessartine. Mi- croprobe data for the Cr-pyrope and eclogitic garnets is shown in Stephenson (1999, Appendix G) and data for the other garnets is shown in Stephenson (1999, Appendix I). Summary statistics for both the raw and normalized Cr-pyrope data are summarized in Table 3. Distribution diagrams based on the raw Cr-pyrope garnet data (Figure 8) and the normalized Cr-pyrope data (Figure 9), both show 4 areas where anomalous or elevated concentrations of “G10” and “G9” Cr-pyrope garnets occur. These areas are: 1) Mattawitchewan River (114-MA-98); 2) Goat River (30-MA-98, 31-MA-98, 32-MA-98, 33-MA-98); 3) North Brunswick River (38-MA-98, 76-MA-98, 77-MA-98, 82-MA-98); and 4) Missinaibi River-Opasatika Lake (85-GL-98, 91-MA-98, 95-MA-98, 96-MA-98, 99-MA-98, 103-MA-98, 104-MA-98, 107-MA-98, 108-MA-98, 150-TM-98, 155-TM-98). Although “G10” garnet data has been normalized, care should be exercised in using this data given the rarity and low numbers of these grains.

Data for the four eclogitic garnets was plotted on a wt % TiO2 versus wt % Na2O plot (Figure 10). One grain, 102-MA-98 has elevated sodium concentrations (> 0.7 wt % Na2O) (Fipke et al. 1995) indicating a possible kimberlitic source. All four eclogitic garnets occur in modern alluvium samples obtained from the eastern part of the field area (75-MA-98 from the Missinaibi River area; 89-MA-98 from the Opasatika River area; and 102-MA-98, and 103-MA-98 from the Opasatika Lake area). Chromite One hundred and eighteen chromite grains were submitted to the OGC for microprobe analysis (Stephen- son 1999, Appendix G). One grain was lost in the preparation of the plugs, 8 grains were identified as non- chromites and 2 grains were determined to be ilmenites (33-MA-98-CR 40 and 116-MA-98-CR 93). None of the chromite grains plot in the inclusion field of Fipke et al. (1995) (Figure 11) and only 2 grains (18-MA-98-CR 7 and 151-TM-98-CR 116) plot in the field unique to kimberlite and lamproite on a wt % TiO2 vs. wt % Cr2O3 plot (Figure 12). Ten grains plot in the non-lamproitic/kimberlitic field and were excluded from the KIM data set (Stephenson 1999, Appendix I). The remaining 99 grains plot in the overlap field and were included in the KIM data set (Stephenson 1999, Appendix G). Summary statistics for the chromite data are summarized in Table 3.

11 12 13 14 Table 3. Summary statistics for KIMs. Data is presented as raw data (R) and as normalized data (N) (see “Data Plotting Parameters”). Percentile thresholds are used for Figures 20 and 21.

Media General Statistics Percentile Statistics Total Grains Maximum 95th 90th 75th 50th R N R N R N R N R N R N Modern Alluvium “G10”s 3 6 2 4 0 0 0 0 0 0 0 0 “G9”s 28 54 3 6 1 2 1 2 0 0 0 0 Chromite 131 249 26 56 7 15 2 4 1 1 0 0 Mg-ilmenite 32 61 5 10 2 4 1 2 0 0 0 0 Cr-diopside 26 46 4 6 1 2 1 2 0 0 0 0 Percentile Threshold 9 21 4 7 2 3 0 0

Glaciolacustrine “G10”s 0 0 0 0 0 0 0 0 0 0 0 0 “G9”s 1 2 1 2 1 1 0 0 0 0 0 0 Chromite 12 20 10 16 6 9 1 2 1 1 0 0 Mg-ilmenite 2 4 1 2 1 2 1 2 0 0 0 0 Cr-diopside 2 3 1 2 1 1 1 1 0 0 0 0 Percentile Threshold 6 10 1 2 1 2 1 0

Till “G10”s 0 0 0 0 0 0 0 0 0 0 0 0 “G9”s 6 6 1 1 1 1 1 1 0 0 0 0 Chromite 5 5 1 1 1 1 1 1 0 0 0 0 Mg-ilmenite 9 9 3 3 1 1 1 1 1 1 0 0 Cr-diopside 3 3 1 1 1 1 1 1 0 0 0 0 Percentile Threshold 3 3 2 3 1 1 1 1 Distribution diagrams using raw chromite data (Figure 13) and normalized chromite data (Figure 14) both show 4 areas of chromite concentrations. The 4 areas are: 1) Mattawitchewan River (114-MA-98, 115-MA-98, 116-MA-98); 2) Goat River (8-MA-98, 20-MA-98, 21-GL-98, 25-MA-98, 29-MA-98, 30-MA-98, 31-MA-98, 32-MA-98, 33-MA-98, 37-MA-98); 3) Missinaibi-Brunswick River (42-MA-98, 45-MA-98, 46-MA-98, 74-MA-98, 76-MA-98, 78-MA-98, 82-MA-98, 94-MA-98, 106-MA-98, 136-TM-98, 143-TM-98, 151-TM-98, 152-TM-98, 155-TM-98); and 4) Rufus Lake (4-GL-98, 85-GL-98, 104-MA-98). Mg-ilmenite Of the 90 ilmenite grains submitted to the OGC for microprobe analysis, 42 were determined to be Mg-ilmenites (Stephenson 1999, Appendix G) and 39 others were identified as ilmenites (Stephenson 1999, Ap- pendix I). One grain was identified as a chromite (116-MA-98-IM 55) and 8 grains were determined to be non-ilmenites. Summary statistics for Mg-ilmenite data are summarized in Table 3. Data for 43 Mg-ilmenites was plotted on Gurney and Moore’s (1991) Mg-ilmenite parabolic plot. Fourteen grains fall in the reducing part of the diagram suggesting favourable conditions for diamond preservation within the magma. Fifteen grains fall in the oxidizing area of the plot, an environment where diamonds are reabsorbed into the magma (Figure 15, Table 4). The remaining 14 grains fall outside of the plot.

15 16 17 18 19 20 21 22 23 Table 4. Summary of reduced vs. oxidized environment for Mg-ilmenite grains. A reduced environment is favourable for diamond preservation.

Sample Grain Reduced Oxidized Outside of plot Number Number (Diamond Preservation) (Diamond Readsorption)

GL-7-98 IM-1 X MA-15-98 IM-2 X MA-15-98 IM-3 X MA-19-98 IM-4 X MA-20-98 IM-6 X MA-20-98 IM-7 X MA-29-98 IM-13 X MA-31-98 IM-19 X MA-31-98 IM-23 X MA-31-98 IM-24 X MA-31-98 IM-25 X MA-31-98 IM-26 X MA-33-98 IM-27 X MA-33-98 IM-28 X MA-33-98 IM-29 X MA-33-98 IM-30 X MA-33-98 IM-31 X MA-38-98 IM-32 X MA-45-98 IM-34 X MA-49-98 IM-41 X GL-50-98 IM-42 X MA-70-98 IM-44 X MA-97-98 IM-47 X MA-104-98 IM-48 X MA-104-98 IM-49 X MA-104-98 IM-50 X MA-105-98 IM-51 X MA-106-98 IM-52 X MA-106-98 IM-53 X MA-106-98 IM-54 X MA-116-98 IM-56 X MA-116-98 CR-93 X MA-120-98 IM-58 X MA-120-98 IM-59 X TM-135-98 IM-69 X TM-136-98 IM-70 X TM-138-98 IM-71 X TM-138-98 IM-72 X TM-138-98 IM-73 X TM-143-98 IM-74 X TM-144-98 IM-75 X TM-148-98 IM-76 X TM-152-98 IM-77 X

24 There are 4 areas where anomalous concentrations of Mg-ilmenites occur based on both the raw data for Mg-ilmenites (Figure 16) and the normalized data (Figure 17): 1) Goat River (7-GL-98, 19-MA-98, 20-MA-98, 29-MA-98, 31-MA-98, 33-MA-98); 2) Brunswick River (70-MA-98, 135-TM-98, 136-TM-98, 138-TM-98, 143-TM-98, 148-TM-98, 152-TM-98); 3) Missinaibi River (45-MA-98, 97-MA-98, 106-MA-98); and 4) Rufus Lake (104-MA-98, 105-MA-98). Cr-diopside One hundred and ninety-seven Cr-diopsides were submitted to the OGC for microprobe analysis. One grain was lost in preparation of the plugs. Of the grains submitted for analysis, 29 have greater than 1 wt % Cr2O3 (Stephenson 1999, Appendix G), 163 have less than 1 wt % Cr2O3 (Stephenson 1999, Appendix I) and 4 were determined not to be Cr-diopside. Summary statistics for the Cr-diopside data are summarized in Table 3. There are 3 areas where anomalous concentrations of Cr-diopside occur based on both the raw data for Cr-diopside (Figure 18) and the normalized data (Figure 19). These areas are: 1) Mattawitchewan River (14-MA-98, 15-MA-98, 110-MA-98, 117-MA-98, 121-MA-98); 2) Goat River (10-MA-98, 20-MA-98); and 3) Missinaibi-Brunswick River area (45-MA-98, 99-MA-98, 107-MA-98, 156-TM-98). Recommendations for Kimberlite Exploration In examining the distribution and compositions of individual KIMs, several sites and related areas were identified as favourable for kimberlite exploration. However, by considering the total number of KIMs for each site, fewer exploration targets of higher quality can be recommended. This may be more desirable in that the recommended exploration areas would be based on sample sites containing significant KIMs (e.g., a “G10”) or a variety of KIMs (e.g., a “G10”, Mg-ilmenite and chromite). The recommendations for exploration are based on distribution diagrams of total KIMs at each sample site using both raw data (Figure 20) and normalized data (Figure 21). Five areas and several individual sites are recommended for kimberlite exploration (Table 5, Table 6). Estimating proximity of KIM signature to source is difficult given the glacial history of the area. How- ever, the pebble data may be useful. A sample site with a predominantly local mix of pebbles (granite, gneiss, metavolcanics, metasediments), as opposed to pebbles derived from more distal sources (carbon- ates, sandstones), may suggest a relatively close proximity to source (Table 5, Table 6). For example, the 2 sites where the “G10” Cr-pyrope garnets were recovered (114-MA-98 and 14-MA-98) both have relatively low percentages of exotic pebbles suggesting a close proximity to source. Aeromagnetic data may also be useful in evaluating the proximity of KIMs to source (Geological Sur- vey of Canada 1963a, 1963b). Samples with anomalous values of KIMs close to a circular-ellipsoid magnetic signature (Morris and Kaszycki 1997) suggests proximity to a potential source. For example, sites 14-MA-98, 15-MA-98, 38-MA-98, 102-MA-98, and 116-MA-98 each have ellipsoid magnetic depressions nearby while sites 37-MA-98, 82-MA-98 and 114-MA-98 occur near positive ellipsoid magnetic anomalies. Structural data may also be useful. Several anomalous sites occur at or near the intersections of dikes and lineaments (31-MA-98, 32-MA-98, 33-MA-98, 114-MA-98, 116-MA-98) or along the fault controlled Opasatika Lake-Rufus Lake drainage (99-MA-98, 102-MA-98, 103-MA-98, 104-MA-98). Close proximity to source is also suggested by the presence of Cr-diopside (Stephenson 1999, Appen- dix G) and olivine (21-GL-98, 38-MA-98, 56-MA-98, 58-MA-98, 73-MA-98, 85-GL-98) since these minerals break down very easily in the surface environments (Felix Kaminsky, KM Diamond Exploration Ltd., personal communication, 1998).

25 26 27 28 29 30 31 32 33 METAMORPHOSED MAGMATIC/MASSIVE SULPHIDE INDICATOR MINERALS The number and type of MMSIM’s picked are summarized in Stephenson (1999, Appendix F). Summary statistics for both the raw MMSIM data and normalized MMSIM data are given in Table 7. The microprobe analysis data for MMSIMs including gahnite, low Cr-diopside, chromite and olivine is presented in Ste- phenson (1999, Appendix H) and the data for low-chrome chromite is presented in Stephenson (1999, Ap- pendix I). Gahnite Ten gahnite grains were submitted to the OGC for microprobe analysis. Of these, 9 were identified as gahnite (Stephenson, 1999, Appendix H). The distribution of gahnite grains in the field area based on the raw data is shown on Figure 22 while the distribution based on normalized data is shown on Figure 23. The molecular weight percent of the composition of the gahnite grains were calculated as per Morris et al. (in press) and plotted on a ternary diagram (Figure 24). Two distinct groups are evident:

Group 1: Contains 2 grains (25-MA-98, 125-MA-98) with normalized 0.5 to 0.8 wt % MgO, normalized 73 to 87 wt % ZnO and normalized 12 to 26 wt % FeO. This group corresponds well with the composition of gahnite recovered from pegmatite in the Separation Lake area and to similar composition fields of gahnite recovered from till samples collected in the Separation Lake area and from modern alluvium samples collected in the Kinniwabi Lake and Kapuskasing areas (Morris 1996a, Morris 1997, Morris 1998). Group 2: Contains 7 grains with normalized 1 to 14 wt % MgO, normalized 67 to 82 wt % ZnO and normalized 12 to 23 wt % FeO. This group corresponds well with the composition of gahnite recovered from various polymetallic deposits in Ontario (Geco, Mattabi) and the USA (Mineral Ridge District, Virginia). In addition, the data is comparable to the composition of gahnite grains from till samples collected in the Separation Lake area and from modern alluvium samples collected in the Kinniwabi Lake and Kapuskasing areas (Morris 1996a, Morris 1997, Morris 1998). The distribution of these 2 different groups is illustrated in Figure 25. The pegmatitic gahnites seem to form a northwest-southeast distribution pattern and may be sourced from pegmatitic veins in the muscovite granite. Ruby Corundum Fourteen ruby corundum grains were submitted for microprobe analysis. Of these, 13 were identified as ruby corundum. The compositions of the ruby corundum grains are presented in Stephenson (1999, Appen- dix H).

34 Table 7. Summary statistics for MMSIMs. Data is presented as raw data (R) and as normalized data (N) (see “Data Plotting Parameters”). Percentile thresholds are used for Figures 26 and 27.

Media General Statistics Percentile Statistics Total Grains Maximum 95th 90th 75th 50th R N R N R N R N R N R N Modern Alluvium Staurolite 1 2 1 2 0 0 0 0 0 0 0 0 Anthophyllite 0 0 0 0 0 0 0 0 0 0 0 0 Hypersthene 0 0 0 0 0 0 0 0 0 0 0 0 Olivine 6 10 2 3 0 0 0 0 0 0 0 0 Spessartine 1 2 1 2 0 0 0 0 0 0 0 0 Red Epidote 16 30 2 4 1 2 1 2 0 0 0 0 Sapphirine 1 2 1 2 0 0 0 0 0 0 0 0 Chromite 137 260 26 56 7 15 2 4 1 2 0 0 Red Rutile 40 81 9 19 2 3 1 2 0 0 0 0 Ruby Corundum 10 18 1 2 1 2 0 0 0 0 0 0 Gahnite 9 16 1 3 1 2 0 0 0 0 0 0 Chalcopyrite 110 210 9 20 4 7 3 6 1 2 0 0 Cr-diopside 118 210 7 15 3 6 3 5 2 3 0 0 Percentile Threshold 14 24 7 16 5 9 2 4 Glaciolacustrine Staurolite 0 0 0 0 0 0 0 0 0 0 0 0 Anthophyllite 0 0 0 0 0 0 0 0 0 0 0 0 Hypersthene 2 4 1 2 1 2 1 2 0 0 0 0 Olivine 2 4 1 2 1 2 1 2 0 0 0 0 Spessartine 0 0 0 0 0 0 0 0 0 0 0 0 Red Epidote 1 2 1 2 1 1 0 0 0 0 0 0 Sapphirine 2 4 1 2 1 2 1 2 0 0 0 0 Chromite 14 24 10 16 2 10 2 5 1 2 0 0 Red Rutile 21 34 11 17 7 11 2 5 2 3 1 2 Ruby Corundum 1 1 1 1 1 1 0 0 0 0 0 0 Gahnite 1 2 1 2 1 1 0 0 0 0 0 0 Chalcopyrite 5 8 2 3 2 3 2 3 1 1 0 0 Cr-diopside 16 25 7 11 6 9 4 6 3 4 0 0 Percentile Threshold 19 30 17 27 6 13 3 7 Till Staurolite 5 5 2 2 2 2 1 1 0 0 0 0 Anthophyllite 0 0 0 0 0 0 0 0 0 0 0 0 Hypersthene 0 0 0 0 0 0 0 0 0 0 0 0 Olivine 0 0 0 0 0 0 0 0 0 0 0 0 Spessartine 21 22 9 9 4 4 2 2 1 1 0 0 Red Epidote 1 1 1 1 0 0 0 0 0 0 0 0 Sapphirine 0 0 0 0 0 0 0 0 0 0 0 0 Chromite 5 5 1 1 1 1 1 1 0 0 0 0 Red Rutile 57 64 20 23 6 8 4 5 3 3 1 1 Ruby Corundum 2 2 1 1 1 1 0 0 0 0 0 0 Gahnite 0 0 0 0 0 0 0 0 0 0 0 0 Chalcopyrite 12 13 2 3 2 2 2 2 1 1 0 0 Cr-diopside 30 33 6 8 4 5 3 3 2 2 1 1 Percentile Threshold 16 18 13 16 6 7 4 4

35 36 37 38 39 Olivine Eight olivine grains were submitted for microprobe analysis. Of these, 7 were identified as fayolitic olivine and 1 was identified as andradite. The compositions of the olivine grains are presented in Stephenson (1999, Appendix H). Recommendations for Massive Sulphide Exploration Like the KIM data, examination of the distribution of individual MMSIMs identified several sites and related areas favorable for massive sulphide exploration. However, by considering the total number of MMSIMs present at each site fewer exploration targets of higher quality can be recommended. This may be more desirable in that the recommended exploration areas are based on sample sites containing a significant MMSIM (e.g., a gahnite) or a variety of MMSIMs (e.g., gahnite, chalcopyrite, Cr-diopside ). The recommendations for exploration are based on distribution diagrams of total MMSIMs at each sample site using both raw data (Figure 26) and normalized data (Figure 27). Three areas and several individual sites are recommended for massive sulphide exploration (Table 8, Table 9). Estimating proximity of an MMSIM signature to source is difficult given the glacial history of the area. Using pebble data, however, may be useful (see KIM discussion) in locating a source. In addition, the presence of olivine (21-MA-98, 38-MA-98, 56-MA-98, 58-MA-98, 73-MA-98, 85-GL-98) also suggests close sample site proximity to source, as olivine breaks down easily in the surface environment. As with the KIMs, the presence of Cr-diopside (Stephenson 1999, Appendix H) may also suggest close proximity to source (Felix Kaminsky, KM Diamond Exploration Ltd., personal communication, 1998). Aeromagnetic data may also be useful in determining site proximity to source. Samples with anomalous values of MMSIMs close to a positive magnetic signature may suggest proximity to a potential source. Samples 31-MA-98, 33-MA-98, 93-MA-98, 114-MA-98, 116-MA-98, and 152-TM-98 all occur above or just down-ice from strong linear positive magnetic anomalies.

40 41 42 43 44 GOLD GRAINS The number of gold grains recovered in this study is small relative to other studies completed in northeastern Ontario (Bajc 1994, Bernier 1994). This is reflected by the very low value for the 95th percentile; the parameters used to define the limit of anomalous concentrations of gold grains (Table 10).

The majority of gold grains recovered were reshaped, suggesting some distance of transport (Table 10). However, one modern alluvium sample (106-MA-98) had one pristine grain suggesting close proximity to source. Three areas, all in the eastern portion of the field area, showed anomalous (>95th percentile) or elevated (> 90th percentile) concentrations of gold grains. The distribution diagram based on the raw data for total gold grains is presented as Figure 28 and the distribution diagram based on the normalized gold data is presented as Figure 29. These areas and individual sample sites are summarized in Table 11 and Table 12 . These anomalous areas are supported by a good correlation with the distribution of chalcopyrite grains. However, given the low number of gold grains found in these areas, the value of these areas as exploration targets may be low. The gold in the south Missinaibi River area is most likely associated with the Rufus Lake fault system and the faulting west of Brunswick Lake. The concentration of gold in the Fergus Road area is down ice from a strong positive magnetic anomaly possibly representing an alkalic intrusion which may be associated with the gold (Ben Berger, Ontario Geological Survey, personal communication, 1999).

45 46 47 48 Acknowledgements The authors would like to thank Sylvie Handley (Northern Development Officer, Ministry of Northern De- velopment and Mines, Kapuskasing), Tom Mispel-Beyer (Area Supervisor, Ministry of Natural Resources, Kapuskasing) and Rick Wilkins (Owner, Rufus Lake Lodge) for providing excellent logistical support during the summer field season. Thanks are also extended to Stanley Gerard of Domtar Forest Products for arranging access onto Domtar property in the western part of the field area. Chris Peloso provided excellent field assistance and Shannon Tait drafted all figures in the report. Thanks are extended to Cam Baker for providing a review of this manuscript and for his continuing support of the heavy mineral sampling programs.

49 References

Bajc, A.F. 1994. Gold grains in surface till samples, Parkin and Norman townships, Sudbury; Ontario Geological Survey, Open File Report 5893, 24p.

Batchelor, R.A. and Kinnaird, J.A. 1984. Gahnite compositions compared; Mineralogical Magazine, v.48, p.425-429.

Berger, B.R. 1986. Geology of the Hearst-Kapuskasing area, District of Cochrane; Ontario Geological Survey, Open File Report 5599, 88p.

Bernier, M.A. 1994. Particulate gold and heavy mineral abundance in surficial sediments, western Swayze greenstone belt; Ontario Geological Survey, Open File Report 5898, 63p.

Boland, A.V. and Ellis, R.M. 1989. Velocity structure of the Kapuskasing uplift, northern Ontario, from seismic refrac- tion studies; Journal of Geophysical Research, v.94, n.B6, p.7198-7204.

Bostock, H.S. 1976. Physiographic subdivisions of Canada; in Geology and Economic Minerals of Canada, Part A, Geo- logical Survey of Canada, Economic Report No. 1, p.10-42.

Cerny, P. and Hawthorne, F.C. 1982. Selected peraluminous minerals; MAC short course handbook, v.8, p.163-186.

Cerny, P., Trueman, D.L., Ziehlke, D.V., Goad, B.E. and Paul, B.J. 1981. The Cat Lake-Winnipeg River and the Wekusko Lake pegmatite fields, Manitoba; Manitoba Department of Energy and Mines, Mineral Resources Division, Eco- nomic Report ER80-1, 234p.

Chew, K.J. 1977. The origin of certain base metal sulphide deposits at Manitouwadge, Ontario; unpublished PhD. thesis, University of Aberdeen, Aberdeen, United Kingdom, 254p.

Dawson, J.B. and Stephens, W.E. 1975. Statistical classification of garnets from kimberlite and associated xenoliths; Journal of Geology, v.83, no.5, p.589-607.

DiLabio, R.N.W. 1990. Classification and interpretation of the shapes and surface textures of gold grains from till on the Canadian Shield; in Current Research, Part C, Geological Survey of Canada, Paper 90-1c, p.323-329.

Fipke, C.E., Gurney, J.J. and Moore R.O. 1995. Diamond exploration techniques emphasizing indicator mineral geo- chemistry and Canadian examples; Geological Survey of Canada Bulletin 423, 86p.

Geological Survey of Canada, 1963a. Opasatika Lake, Algoma and Cochrane Districts, Ontario, Aeromagnetic series map 2237G, scale 1:63,360.

Z 1963b. Goat River, Algoma and Cochrane Districts, Ontario, Aeromagnetic series map 2223G, scale 1:63,360.

Gurney, J.J. 1984. A correlation between garnets and diamonds in kimberlite; in Kimberlite occurrence and origin: a basis for conceptual models in exploration, University of Western Australia, Perth, Western Australia, Publication no. 8, p.143-166.

Gurney, J.J. and Moore, R.O. 1991. Kimberlite garnet, chromite and ilmenite compositions, applications to exploration. in P.Sheahan and A.Chater (Editors), Diamonds: exploration, sampling and evaluation; Prospectors and Developers Association of Canada, Toronto, pp.109-146.

Lalonde, J.P., Bernier, L., Choinier, J. and Hebert, C. 1994. Dispersion of gahnite from the Montauban and Lac Dussault polymetallic deposits, Portneuf Township, Quebec; Ministere des Ressources Naturelles, Secteur des Mines, MB 94-41, 39p.

Matile, G.L.D. and Thorliefson, L.H. 1997. Till geochemical and indicator mineral reconnaissance of northeastern Man- itoba; Manitoba Energy and Mines, Open File OF97-3, 174p.

McCallum, M.E. and Vos, W.P. 1993. Ilmenite signatures: utilization of paramagnetic and geochemical properties in kimberlite exploration; in Diamonds: exploration, sampling and evaluation, proceedings of a short course presented by the Prospectors and Developers Association of Canada, Toronto, Ontario, 1993, p.109-146.

50 Morris, T.F. 1990. Quaternary geology of the Wawa area, northern Ontario; in Summary of Field Work and Other Activi- ties 1990, Ontario Geological Survey, Miscellaneous Paper 151, p.149-151.

Z 1991. Quaternary geology of the Wawa area, northern Ontario; in Summary of Field Work and Other Activities, 1991, Ontario Geological Survey, Miscellaneous Paper 157, p.149-151.

Z 1992a. Quaternary geology of the Wawa area; Ontario Geological Survey, Open File Map 192, scale 1:50 000.

Z 1992b. Quaternary geology, Dog Lake area, northern Ontario; Ontario Geological Survey, Open File Map 199, scale 1:50 000.

Z 1994a. Quaternary geology and overburden sampling for kimberlite indicators in the Michipicoten River-Wawa area, northeastern Ontario; in Summary of Field Work and Other Activities 1994, Ontario Geological Survey, Miscella- neous Paper 163, p.247-249.

Z 1994b. Results of overburden sampling for kimberlite indicator minerals and gold grains, Michipicoten River-Wawa area, northeastern Ontario; Ontario Geological Survey, Miscellaneous Release - Data 13.

Z 1995a. Michipicoten River-Wawa kimberlite heavy mineral study; in Summary of Field Work and Other Activities, Ontario Geological Survey, Miscellaneous Paper 164, p.271

Z 1995b. Kimberlite, base metal and gold exploration using overburden, Wawa area; in Institute on Lake Superior Geol- ogy, 41st Annual Meeting, May 13-18, 1995, Marathon, Ontario, Proceedings Volume 41: Part 2e Field Trip Guide- book, 62p.

Z 1996a. Quaternary mapping and overburden sampling for kimberlite indicator minerals, Kinniwabi Lake area, northeastern Ontario; in Summary of Field Work and Other Activities, Ontario Geological Survey, Miscellaneous Paper 166, p.191-193.

Z 1996b. Geochemical and heavy mineral data, surficial sediment sampling program, Separation Lake area, northwestern Ontario; Ontario Geological Survey, Open File Report 5939, 44p.

Z 1997a. Quaternary geology mapping and overburden sampling, Woman Falls - Wakusimi River area, northeastern Ontario; in Summary of Field Work and Other Activities, Ontario Geological Survey, Miscellaneous Paper 168, p.113-115.

Z 1997b. Results of modern alluvium sampling for kimberlite indicator minerals and gahnite, Kinniwabi Lake area, northeastern Ontario; Ontario Geological Survey, Miscellaneous Release - Data 23.

Z 1998. Kimberlite, base metal and gold exploration targets based upon heavy mineral data derived from surficial deposits, Kapuskasing area, northeastern Ontario; Ontario Geological Survey, Miscellaneous Release - Data 34.

Morris, T.F. and Kaszycki, C.A. 1997. Prospector’s guide to drift prospecting for diamonds, northern Ontario; Ontario Geological Survey, Miscellaneous Paper 167, 63p.

Morris, T.F., Crabtree, D.C. and Averill, S.A. 1998. Kimberlite, base metal and gold exploration targets based upon heavy mineral data derived from surface materials, Kapuskasing, northeastern Ontario; Ontario Geological Survey, Open File Report 5967, 42p.

Morris, T.F., Crabtree, D. and Pianosi, S. 1997. Results of modern alluvium sampling for kimberlite indicator minerals, Kinniwabi Lake area, northeastern Ontario; Ontario Geological Survey, Open File Report 5956, 72p.

Morris, T.F., Murray, C. and Crabtree, D. 1994. Results of overburden sampling for kimberlite indicator minerals and gold grains, Michipicoten River-Wawa area, northeastern Ontario; Ontario Geological Survey, Open File Report 5908, 69p.

Morris, T.F., Crabtree, D.C., Sage, R.P., and Averill, S.A. 1998. Types, abundances and distribution of kimberlite indicator minerals in alluvial sediments, Wawa-Kinniwabi Lake area, Northeastern Ontario: implications for the presence of diamond-bearing kimberlite; Journal of Geochemical Exploration, v.63, p.217-235.

51 Morris, T.F., Breaks, F.W., Averill, S.A., Crabtree, D.C. and McDonald, A., in press. Gahnite Composition: Implications for base metal and rare-element exploration; Exploration and Mining Geology.

Ontario Geological Survey, 1991. Bedrock geology of Ontario, east-central sheet: Ontario Geological Survey, Map 2543, scale 1:1 000 000.

Parr, J. 1992. A gahnite-garnet retrograde reaction from the Pinnacles deposit, Broken Hill, New South Wales, Australia; Canadian Mineralogist, v.30, p.145-152.

Plimer, I.R. 1977. The mineralogy of the high grade metamorphic rocks enclosing the Broken Hill orebodies, Australia; NeusesJahrbuch fur Mineralogie Abhandlungen, v.131, p.115-139.

Sheridan, D.M. and Raymond, W.H. 1984. Preliminary data on some Precambrian deposits of zinc-copper-lead sulphides and zinc spinel (gahnite) in Colorado; United States Geological Survey Open File Report 77, 607p.

Spry, P.G. 1982. An unusual gahnite-forming reaction, Geco base metal deposit, Manitouwadge, Ontario; Canadian Min- eralogist, v.20, p.549-553.

Spry, P.G. 1987a. Compositional zoning in zincian spinels; Canadian Mineralogist, v.25, p.97-104.

Z1987b. The chemistry and origin of zincian spinel associated with the Aggeneys Cu-Pb-Zn-Ag deposits, Namaqual- and, South Africa; Mineralium Deposita, v.22, p.262-268.

Spry, P.G. and Scott, S.D. 1986. The stability of zincian spinels in sulphide systems and their potential as exploration guides for metamorphosed massive sulphide deposits; Economic Geologist, v.81, p.1446-1463.

Stephenson, D.M. 1999. Kimberlite, base metal and gold exploration targets based upon heavy mineral data derived from surface materials, Opasatika Lake area, northeastern Ontario; Ontario Geological Survey, Miscellaneous Release - Data 41.

Williams, P.J. 1983. The mineralogy and metamorphism of some gahnite-bearing silicate intrusions in massive sulphides from Fornas, northwest Spain; Mineralogy Magazine, v.47, p.233-235.

52 Appendix 1

Sample Site Locations Summary list of abbreviations: GL: glaciolacustrine sample GLP: glaciolacustrine pebble sample MA: modern alluvium sample MAP: modern alluvium pebble sample TM: till “C” horizon sample TP: till pebble sample GRN: granite bedrock terrane GTN: gneissic tonalite bedrock terrane MGRN: muscovite-bearing granite terrane MS: metasedimentary bedrock terrane MUM: mafic-ultramafic bedrock terrane MV: mafic metavolcanic bedrock terrane TNL: tonalite bedrock terrane

53 Appendix A: Sample Site Locations Sample U.T.M’s Associated Sample U.T.M’s Associated Number/Material Easting Northing Bedrock Number/Material Easting Northing Bedrock 1--MA--98 346450 5449500 GTN 3 0 -- M A -- 9 8 307560 5455342 MGRN/MS 1--MAP--98 346450 5449500 GTN 30--MAP--98 307560 5455342 MGRN/MS 2--MA--98 345900 5450550 GTN 3 1 -- M A -- 9 8 308360 5457066 MS 2--MAP--98 345900 5450550 GTN 31--MAP--98 308360 5457066 MS 3--MA--98 344850 5452000 GTN 3 2 -- M A -- 9 8 309659 5457500 MS 4--GL--98 344250 5452400 GTN 32--MAP--98 309659 5457500 MS 4--GLP--98 344250 5452400 GTN 3 3 -- M A -- 9 8 308754 5456560 MGRN/MS 5--MA--98 323129 5445531 GTN/MUM 33--MAP--98 308754 5456560 MGRN/MS 5--MAP--98 323129 5445531 GTN/MUM 3 4 -- M A -- 9 8 308118 5455038 MS 6--MA--98 321030 5449135 MS 3 5 -- M A -- 9 8 306561 5450734 MV 7--GL--98 306822 5448920 MUM 3 6 -- M A -- 9 8 305360 5456541 MV/MGRN 7--GLP--98 306822 5448920 MUM 36--MAP--98 305360 5456541 MV/MGRN 8--MA--98 306653 5449498 MUM 3 7 -- M A -- 9 8 311226 5449389 MV 8--MAP--98 306653 5449498 MUM 37--MAP--98 311226 5449389 MV 9--MA--98 307477 5454490 MS 3 8 -- M A -- 9 8 320200 5456021 MS 1 0 -- M A -- 9 8 297952 5437525 GTN 38--MAP--98 320200 5456021 MS 10--MAP--98 297952 5437525 GTN 3 9 -- G L -- 9 8 320378 5454338 MS 1 1 -- M A -- 9 8 296855 5436822 GTN 39--GLP--98 320378 5454338 MS 1 2 -- M A -- 9 8 295892 5437464 MGRN 4 0 -- M A -- 9 8 318759 5451614 MV 12--MAP--98 295892 5437464 MGRN 40--MAP--98 318759 5451614 MV 1 3 -- G L -- 9 8 295804 5435550 GTN 4 1 -- M A -- 9 8 318418 5450875 MV 13--GLP--98 295804 5435550 GTN 4 2 -- M A -- 9 8 322639 5444884 GTN 1 4 -- M A -- 9 8 294774 5432855 GTN/MV 42--MAP--98 322639 5444884 GTN 14--MAP--98 294774 5432855 GTN/MV 4 3 -- M A -- 9 8 324180 5447719 GTN 1 5 -- M A -- 9 8 297375 5431410 MV 4 4 -- M A -- 9 8 324225 5447350 GTN 15--MAP--98 297375 5431410 MV 4 5 -- M A -- 9 8 335150 5435755 TNL 1 6 -- G L -- 9 8 302102 5435168 GTN 45--MAP--98 335150 5435755 TNL 16--GLP--98 302102 5435168 GTN 4 6 -- M A -- 9 8 335290 5436611 TNL 1 7 -- M A -- 9 8 301718 5434893 GTN 46--MAP--98 335290 5436611 TNL 17--MAP--98 301718 5434893 GTN 4 7 -- M A -- 9 8 321527 5433630 TNL 1 8 -- M A -- 9 8 300365 5438854 GTN 4 8 -- M A -- 9 8 319884 5435631 MS 18--MAP--98 300365 5438854 GTN 4 9 -- M A -- 9 8 320193 5435460 MS 1 9 -- M A -- 9 8 310240 5446517 MS 49--MAP--98 320193 5435460 MS 19--MAP--98 310240 5446517 MS 5 0 -- G L -- 9 8 321075 5435762 MS 2 0 -- M A -- 9 8 303453 5445388 GTN 50--GLP--98 321075 5435762 MS 20--MAP--98 303453 5445388 GTN 5 1 -- M A -- 9 8 332422 5447689 GTN 2 1 -- G L -- 9 8 304200 5446027 GTN 5 2 -- M A -- 9 8 345895 5456386 MS 21--GLP--98 304200 5446027 GTN 52--MAP--98 345895 5456386 MS 2 2 -- M A -- 9 8 306445 5448082 MV 5 3 -- M A -- 9 8 335547 5447852 GTN 2 3 -- M A -- 9 8 304401 5451197 MV 5 4 -- M A -- 9 8 338067 5445826 GTN 2 4 -- M A -- 9 8 299710 5445627 GTN 54--MAP--98 338067 5445826 GTN 24--MAP--98 299710 5445627 GTN 5 5 -- G L -- 9 8 342345 5447738 GTN 2 5 -- M A -- 9 8 299626 5445515 GTN 55--GLP--98 342345 5447738 GTN 25--MAP--98 299626 5445515 GTN 5 6 -- M A -- 9 8 341106 5451910 GTN 2 6 -- M A -- 9 8 301096 5447255 MV 5 7 -- M A -- 9 8 309820 5432629 GTN 2 7 -- M A -- 9 8 301454 5448361 MUM 57--MAP--98 309820 5432629 GTN 2 8 -- M A -- 9 8 301831 5448801 MUM 5 8 -- M A -- 9 8 318877 5431088 MS 2 9 -- M A -- 9 8 303247 5449440 MUM 58--MAP--98 318877 5431088 MS 29--MAP--98 303247 5449440 MUM 5 9 -- M A -- 9 8 310458 5431981 MV 59--MAP--98 310458 5431981 MV 89--MAP--98 352522 5452804 MV

54 Appendix A: Sample Site Locations Sample U.T.M’s Associated Sample U.T.M’s Associated Number/Material Easting Northing Bedrock Number/Material Easting Northing Bedrock 6 0 -- M A -- 9 8 309506 5435073 GTN 9 0 -- M A -- 9 8 348127 5443400 GTN 6 1 -- G L -- 9 8 344915 5431051 GTN 90--MAP--98 348127 5443400 GTN 61--GLP--98 344915 5431051 GTN 9 1 -- M A -- 9 8 346125 5445902 GTN 6 2 -- M A -- 9 8 349716 5449897 MV 9 2 -- M A -- 9 8 346313 5446155 GTN 6 3 -- M A -- 9 8 330191 5456189 MS 9 3 -- M A -- 9 8 338649 5430239 GTN 6 4 -- M A -- 9 8 332962 5452997 MS 9 4 -- M A -- 9 8 337131 5433622 GTN 64--MAP--98 332962 5452997 MS 94--MAP--98 337131 5433622 GTN 6 5 -- M A -- 9 8 333194 5448596 GTN 9 5 -- M A -- 9 8 337483 5434100 GTN 6 6 -- M A -- 9 8 327402 5431520 TNL 9 6 -- M A -- 9 8 338575 5435159 TNL 6 7 -- M A -- 9 8 326988 5432099 TNL 96--MAP--98 338575 5435159 TNL 6 8 -- M A -- 9 8 322871 5436943 MS 9 7 -- M A -- 9 8 339008 5434870 TNL 6 9 -- M A -- 9 8 326263 5435000 TNL 97--MAP--98 339008 5434870 TNL 69--MAP--98 326263 5435000 TNL 9 8 -- M A -- 9 8 340471 5438233 TNL 7 0 -- M A -- 9 8 325359 5443148 MUM 98--MAP--98 340471 5438233 TNL 70--MAP--98 325359 5443148 MUM 9 9 -- M A -- 9 8 339259 5438685 TNL 7 1 -- G L -- 9 8 325641 5441595 GTN 99--MAP--98 339259 5438685 TNL 71--GLP--98 325641 5441595 GTN 100--MA--98 352655 5438996 GTN 7 2 -- M A -- 9 8 325286 5444036 MUM 101--MA--98 344955 5446426 GTN 72--MAP--98 325286 5444036 MUM 102--MA--98 342141 5431394 TNL 7 3 -- M A -- 9 8 329502 5444388 GTN 103--MA--98 343090 5442523 GTN 73--MAP--98 329502 5444388 GTN 103--MAP--98 343090 5442523 GTN 7 4 -- M A -- 9 8 327876 5447942 GTN 104--MA--98 348552 5441809 GTN 74--MAP--98 327876 5447942 GTN 104--MAP--98 348552 5441809 GTN 7 5 -- M A -- 9 8 327028 5453050 MV 105--MA--98 347444 5448121 GTN 75--MAP--98 327028 5453050 MV 106--MA--98 332049 5434685 TNL 7 6 -- M A -- 9 8 326904 5452354 MV 106--MAP--98 332049 5434685 TNL 76--MAP--98 326904 5452354 MV 107--MA--98 331856 5436160 TNL 7 7 -- M A -- 9 8 325882 5450987 MS 107--MAP--98 331856 5436160 TNL 7 8 -- M A -- 9 8 325222 5448478 GTN 108--MA--98 331933 5437302 GTN 78--MAP--98 325222 5448478 GTN 108--MAP--98 331933 5437302 GTN 7 9 -- M A -- 9 8 328430 5456190 GTN 109--MA--98 330500 5439670 GTN 8 0 -- M A -- 9 8 328346 5455469 MS 109--MAP--98 330500 5439670 GTN 80--MAP--98 328346 5455469 MS 110--MA--98 282417 5445275 GRN 8 1 -- M A -- 9 8 329176 5454700 MS 1 1 1 -- M A -- 9 8 285496 5448398 GRN 81--MAP--98 329176 5454700 MS 112--MA--98 289102 5448724 MGRN 8 2 -- M A -- 9 8 328131 5453250 MV 112--MAP--98 289102 5448724 MGRN 82--MAP--98 328131 5453250 MV 113--MA--98 289095 5458413 MS 8 3 -- M A -- 9 8 325459 5450103 GTN 114--MA--98 290852 5456028 MS/MGRN 8 4 -- M A -- 9 8 347494 5434611 GTN 114--MAP--98 290852 5456028 MS/MGRN 84--MAP--98 347494 5434611 GTN 115--MA--98 293302 5452877 GRN 8 5 -- G L -- 9 8 345081 5446785 GTN 116--MA--98 294295 5453921 MGRN 85--GLP--98 345081 5446785 GTN 116--MAP--98 294295 5453921 MGRN 8 6 -- M A -- 9 8 351993 5454090 MS 117--MA--98 284092 5440665 MGRN 86--MAP--98 351993 5454090 MS 117--MAP--98 284092 5440665 MGRN 8 7 -- M A -- 9 8 352807 5453313 MS 118--MA--98 285921 5441051 MGRN 87--MAP--98 352807 5453313 MS 118--MAP--98 285921 5441051 MGRN 8 8 -- M A -- 9 8 352807 5453012 MV 119--MA--98 282169 5437000 GTN 8 9 -- M A -- 9 8 352522 5452804 MV+D45 119--MAP--98 282169 5437000 GTN 120--MA--98 283658 5436681 GTN 142--TM--98 324890 5441286 GTN 120--MAP--98 283658 5436681 GTN 142--TP--98 324890 5441286 GTN

55 Appendix A: Sample Site Locations Sample U.T.M’s Associated Sample U.T.M’s Associated Number/Material Easting Northing Bedrock Number/Material Easting Northing Bedrock 121--MA--98 289724 5435775 GTN 143--TM--98 324924 5442007 GTN 121--MAP--98 289724 5435775 GTN 143--TP--98 324924 5442007 GTN 122--MA--98 315045 5436000 GTN 144--TM--98 320468 5438281 GTN/MS 123--MA--98 316617 5444698 GTN 144--TP--98 320468 5438281 GTN/MS 124--MA--98 315257 5442008 GTN 145--TM--98 321370 5441073 GTN 125--MA--98 312634 5437892 GTN 145--TP98 321370 5441073 GTN 125--MAP--98 312634 5437892 GTN 146--TM--98 321825 5442706 GTN 126--MA--98 304387 5433800 GTN 146--TP--98 321825 5442706 GTN 126--MAP--98 304387 5433800 GTN 147--TM--98 324433 5444040 MUM 127--MA--98 294489 5442149 GRN 147--TP--98 324433 5444040 MUM 128--MA--98 296238 5448906 MGRN 148--TM--98 327873 5443964 GTN/MUM 128--MAP--98 296238 5448906 MGRN 148--TP--98 327873 5443964 GTN/MUM 129--MA--98 295502 5457400 MS 149--TM--98 332119 5441526 GTN 129--MAP--98 295502 5457400 MS 149--TP--98 332119 5441526 GTN 130--MA--98 301869 5457268 MS 150--TM--98 328808 5437310 GTN 130--MAP--98 301869 5457268 MS 150--TP--98 328808 5437310 GTN 131--MA--98 315138 5456613 MS 151--TM--98 328240 5438954 GTN 132--MA--98 319626 5445137 GTN 151--TP--98 328240 5438954 GTN 133--MA--98 319124 5437741 GTN 152--TM--98 327869 5441856 GTN 134--MA--98 316478 5432729 GTN 152--TP--98 327869 5441856 GTN 134--MAP--98 316478 5432729 GTN 153--TM--98 327662 5442884 MUM 135--TM--98 327398 5445905 GTN 153--TP--98 327662 5442884 MUM 135--TP--98 327398 5445905 GTN 154--TM--98 334696 5434460 GTN 136--TM--98 324312 5445805 GTN 154--TP--98 334696 5434460 GTN 136--TP--98 324312 5445805 GTN 155--TM--98 335236 5437196 TNL 137--TM--98 322406 5446875 GTN 155--TP--98 335236 5437196 TNL 137--TP--98 322406 5446875 GTN 156--TM--98 333811 5439281 GTN 138--TM--98 322400 5443928 GTN 156--TP--98 333811 5439281 GTN 138--TP--98 322400 5443928 GTN 157--TM--98 333067 5449152 GTN 139--TM--98 322386 5444771 GTN 157--TP--98 333067 5449152 GTN 139--TP--98 322386 5444771 GTN 158--TM--98 321826 5435229 GTN 140--TM--98 323368 5436712 GTN 158--TP--98 321826 5435229 GTN 140--TP--98 323368 5436712 GTN 159--TM--98 328926 5433413 TNL 141--TM--98 324100 5438668 GTN 159--TP--98 328926 5433413 TNL 141--TP--98 324100 5438668 GTN

56 Appendix 2

Sample Normalization Calculations

57 1) Count estimate normalization

For sample 76--MA--98, 4 chromite grains were picked from the concentrate out of an estimated 15 grains. Microprobe analysis confirmed only two of the grains were KIM chromite. Normalization is calculated as follows:

number of normalized grains = (estimated number of grains) x number of KIMs ( number of picked grains )

= (15) x2 (4)

= 8 grains

2) Table feed weight normalization

Example 1: For sample 76-MA-98, the table feed weight was 7.40 kg and 1 Cr-pyrope garnet was picked from the sample. To normalize to a table feed weight of 15 kg the calculation is as follows:

number of normalized grains = ( 15 kg ) x number of picked grains (table feed weight)

=( 15 kg ) x1 (7.40 kg)

= 2 grains

Example 2: For sample 76-MA-98, the count estimate number of normalized grains was used instead of the actual number of picked grains for chromite. To normalize to a table feed weight of 15 kg the calculation is as follows:

number of normalized grains = ( 15 kg ) x number of picked grains (table feed weight)

=( 15 kg ) x8 (7.40kg)

=16grains

58 Metric Conversion Table

Conversion from SI to Imperial Conversion from Imperial to SI SI Unit Multiplied by Gives Imperial Unit Multiplied by Gives LENGTH 1 mm 0.039 37 inches 1 inch 25.4 mm 1 cm 0.393 70 inches 1 inch 2.54 cm 1 m 3.280 84 feet 1 foot 0.304 8 m 1 m 0.049 709 chains 1 chain 20.116 8 m 1 km 0.621 371 miles (statute) 1 mile (statute) 1.609 344 km AREA 1cm@ 0.155 0 square inches 1 square inch 6.451 6 cm@ 1m@ 10.763 9 square feet 1 square foot 0.092 903 04 m@ 1km@ 0.386 10 square miles 1 square mile 2.589 988 km@ 1 ha 2.471 054 acres 1 acre 0.404 685 6 ha VOLUME 1cm# 0.061 023 cubic inches 1 cubic inch 16.387 064 cm# 1m# 35.314 7 cubic feet 1 cubic foot 0.028 316 85 m# 1m# 1.307 951 cubic yards 1 cubic yard 0.764 554 86 m# CAPACITY 1 L 1.759 755 pints 1 pint 0.568 261 L 1 L 0.879 877 quarts 1 quart 1.136 522 L 1 L 0.219 969 gallons 1 gallon 4.546 090 L MASS 1 g 0.035 273 962 ounces (avdp) 1 ounce (avdp) 28.349 523 g 1 g 0.032 150 747 ounces (troy) 1 ounce (troy) 31.103 476 8 g 1 kg 2.204 622 6 pounds (avdp) 1 pound (avdp) 0.453 592 37 kg 1 kg 0.001 102 3 tons (short) 1 ton (short) 907.184 74 kg 1 t 1.102 311 3 tons (short) 1 ton (short) 0.907 184 74 t 1 kg 0.000 984 21 tons (long) 1 ton (long) 1016.046 908 8 kg 1 t 0.984 206 5 tons (long) 1 ton (long) 1.016 046 90 t CONCENTRATION 1 g/t 0.029 166 6 ounce (troy)/ 1 ounce (troy)/ 34.285 714 2 g/t ton (short) ton (short) 1 g/t 0.583 333 33 pennyweights/ 1 pennyweight/ 1.714 285 7 g/t ton (short) ton (short) OTHER USEFUL CONVERSION FACTORS Multiplied by 1 ounce (troy) per ton (short) 31.103 477 grams per ton (short) 1 gram per ton (short) 0.032 151 ounces (troy) per ton (short) 1 ounce (troy) per ton (short) 20.0 pennyweights per ton (short) 1 pennyweight per ton (short) 0.05 ounces (troy) per ton (short)

Note: Conversion factors which arein boldtype areexact. Theconversion factorshave been taken fromor havebeen derived from factors given in the Metric Practice Guide for the Canadian Mining and Metallurgical Industries, pub- lished by the Mining Association of Canada in co-operation with the Coal Association of Canada.

ISSN 0826--9580 ISBN 0--7778--8434--8