

Manitoba
Energy and Mines



















Open File Report OF98-5

Operation Superior: Multimedia Geochemical 
Survey Results from the Edmund Lake and 
Sharpe Lake Greenstone Belts, Northern 
Superior Province, Manitoba (NTS 53K)

by M.A.F. Fedikow, E. Nielsen, G.G. Conley and G.L.D. Matile
Winnipeg, 1998


Energy and Mines	Geological Services

Hon. David Newman	C.A. Kaszycki
Minister	Director

Oliver Boulette
Deputy Minister
This publication is available in large print, audiotape or braille on request. 





TABLE OF CONTENTS
INTRODUCTION	
METHODOLOGY	
DATA DISPLAY	
BEDROCK GEOLOGY AND MINERAL DEPOSITS OF THE 1997 SURVEY AREAS	

	Edmund Lake Belt

	Sharpe Lake Belt
		Mineral Deposits

	Sharpe Lake Belt
		Twin Lakes Au Deposits
		Seeber River Au Deposit (C Zone)

	Edmund Lake Belt
		Little Stull Lake Au Deposits
Figure 1:	Location of the 1997 multimedia geochemical survey.
Figure 2:	Regional geology, and mineral deposits in the 1997 survey area.
Figure 3a:	Regional geology, mineral deposits and multimedia sampling sites in the 1997 survey 	
	area.
Figure 3b:	Mylar sample site location map overlay for the Edmund Lake and Sharpe Lake greenstone 
	belts.
Figure 4:	Gold mineralized zones at the Little Stull Lake deposit.
ACKNOWLEDGMENTS	
REFERENCES	
QUATERNARY GEOLOGY OF THE 1997 SURVEY AREAS	

Stratigraphy

Ice Flow Direction

ROCK GEOCHEMICAL SURVEY

Sample Collection, Preparation and Analysis

Format

Results
		Flow Injection Mercury System (FIMS)
		Instrumental Neutron Activation (INA)
		Inductively Coupled Plasma-Atomic Emission
		Spectrometry (ICP-AES)
		Hydrogen Ion (H+)
		Specific Conductance (Water-Extractable Metal)

Synthesis

	Edmund Lake Belt

	Sharpe Lake Belt

Conclusions and Recommendations

Appendix 1: Outcrop Rock Chip Sample Descriptions
Appendix 2: ICP-AES, H+, K and Hg Analyses
Appendix 3: ICP-AES and Hg (FIMS) Analyses, Multiple Samples
Appendix 4: ICP-AES, H+, K and Hg Percentile Bubble Plots
Appendix 5: INA Analyses
Appendix 6: INA Analyses, multiple samples
Appendix 7: INA Percentile Bubble Plots
TILL GEOCHEMICAL SURVEY	

Introduction

Methods
		Field Methods
		Laboratory Methods

Results
		<2µm Fraction

	Edmund Lake Area

	Sharpe Lake Area
		<63 µm Fraction

	Edmund Lake Area

	Sharpe Lake Area

Synthesis

	Edmund Lake Area

	Sharpe Lake Area

Appendix 1: ICP-AES, Hg (cold vapour - AAS) and As (hydride generation) analyses for the <2 micron size 
fraction of till samples
Appendix 2: ICP-AES, Hg and As percentile bubble plots for the <2 micron size fraction of till samples
Appendix 3: INAA for the <63 micron size fraction of till samples
Appendix 4: INAA percentile bubble plots for the <63 micron size fraction of till samples

B-HORIZON SOIL GEOCHEMICAL SURVEY	

Introduction

	Enzyme Leach

Sample Collection

Sample Preparation and Analysis

Results

	Edmund Lake Belt

	Sharpe Lake Belt

Synthesis

Conclusions

Appendix 1: ICP-MS, H+ and K Analyses
Appendix 2: Duplicate Pair ICP-MS Analyses
Appendix 3: ICP-MS, H+ and K Percentile Bubble Plots
HUMUS GEOCHEMICAL SURVEY	

Sample Collection

Sample Preparation and Analysis

Results

	Edmund Lake Belt

	Sharpe Lake Belt

Synthesis

Conclusions

Appendix 1: ICP-AES, H+, K and Hg Analyses
Appendix 2: Duplicate Pair ICP-AES, H+, K and Hg Analyses
Appendix 3: ICP-AES, H+, K and Hg Percentile Bubble Plots
Appendix 4: INA Analyses
Appendix 5: Duplicate Pair INA Analyses
Appendix 6: INA Percentile Bubble Plots

VEGETATION GEOCHEMICAL SURVEY

Introduction

Sample Collection

Sample Preparation and Analysis

Results

	Ash

	Edmund Lake Belt

	Sharpe Lake Belt

Synthesis

Conclusions

Table 1: Essential and non-essential elements determined by INAA.
Table 2: Essential and non-essential elements determined by ICP-AES

Appendix 1: ICP-AES Analyses - Ashed Samples
Appendix 2:  Duplicate Pair ICP-AES Analyses
Appendix 3:  ICP-AES Percentile Bubble Plots
Appendix 4: INA Analyses - Ashed Samples
Appendix 5: Duplicate Pair INA Analyses
Appendix 6: INA Percentile Bubble Plots

SYNOPSIS

KIMBERLITE INDICATOR MINERAL SURVEY	

Introduction

Sample Collection

Sample Preparation and Analysis

Data Display
PRELIMINARY INTERPRETATION OF THE 1997 KIMBERLITE INDICATOR MINERALS SURVEY	

	Results of 1997 Overburden Sampling

	Edmund Lake Belt

	Sharpe Lake Belt

Table 3:	Guidelines for preliminary mineral identification.
Table 4:	Kimberlite indicator mineral classification.
Table 5:	Summary of the geographic distribution of kimberlite indicator mineral grains

Figure 5:	Regional distribution of chrome spinel grains.
Figure 6:	Regional distribution of chrome diopside grains.
Figure 7:	Regional distribution of titanian chrome pyrope garnet grains.
Figure 8:	Regional distribution of “G9” garnet grains.
Figure 9:	Regional distribution of “G10” garnet grains.
Figure 10:	Regional distribution of magnesian ilmenite grains.
Figure 11:	Regional distribution of kimberlite indicator mineral (KIM) sampling sites and total KIM.

Appendix 1:	Mineral Chemistry (MONOPROS Limited) and classifications.
Appendix 2:	Kimberlite Indicator Mineral Abundances.

INTRODUCTION

In 1996 the Manitoba Geological Services Branch embarked upon a five year program of helicopter- and fixed wing-
assisted multimedia geochemical sampling, designed to assist in the definition of exploration targets and the 
assessment of mineral resource potential in the northern Superior geological province. This initiative has been called 
Operation Superior and preliminary results for the area surveyed in 1996 were released in Fedikow et al. (1997a,b).

The application of belt-scale and regional geochemical surveys to relatively underexplored terrane has been 
extensively documented. Usually these surveys have utilized one or two sampling media, such as soil or rock, with 
generally positive results in reducing large tracts of ground to more localized areas of higher exploration prospectivity. 
Operation Superior belt-scale multimedia geochemical surveys specifically address the relatively underexplored 
Archean greenstone belts in the Superior province of northeastern Manitoba by systematically collecting rock, till, b-
horizon soil, humus and vegetation samples from sample sites established at 1 km centers, within mapped boundaries 
of the greenstone belts. The results of surveys conducted in year two of this project are presented in this report, 
representing geochemical survey results for rock, till, b-horizon soil, humus, and vegetation and kimberlite indicator 
mineral survey results for diamonds, respectively.

One of the non-geochemical benefits of landing a helicopter every 1 km during sampling is the opportunity to make 
geological observations at outcrop sample sites and in areas of recent burn. Forest fires in 1988 and 1989 have 
exposed large areas of outcrop in the northern Superior Province that were covered with vegetation and/or soil. An 
excellent example of this benefit has been described in Fedikow et al., (1997a, b) and Fedikow and Nielsen (1997), 
where an areally extensive, highly altered base and precious metal depositional environment was recognized.

A complimentary project was initiated by the Geological Survey of Canada, in 1996. In the federal government survey, 
which focussed on the predominantly intrusive geological terrane separating the greenstone belts, till samples were 
collected on a 40 km sample spacing to provide a regional framework for interpretation of the more detailed multimedia 
program. This survey was undertaken by Harvey Thorleifson of the Geological Survey of Canada and Gaywood Matile 
of the Manitoba Geological Services Branch and has been released as Open File Report OF97-3.

Historically, the commodity focus in Manitoba has focussed on base and precious metals with lesser interest in the 
pegmatite-hosted rare element deposits such as those at Bernic Lake. This multimedia geochemical survey is 
designed to address base and precious metals, pegmatite and carbonatite-hosted rare element deposits as well as 
diamonds. The approach is to collect a variety of sample media at each site and analyze these samples in a multi-
element manner using the most advanced technological instrumentation and innovative digestion techniques available. 
Instrumental neutron activation, (INA) inductively coupled plasma-atomic emission spectrometry (ICP-AES) and 
inductively coupled plasma-mass spectrometry (ICP-MS) are the main analytical techniques chosen for this purpose. 
Additionally, pH and conductivity measurements, converted to H+ and specific conductance respectively, represent 
water-extractable components in rock, b-horizon soil and humus samples and are also examined in this survey.  The 
pH measurements were done using a VWR model 8000 pH meter with a Ross #8165 BN Combination pH electrode. 
Conductivity was measured with an Orion model 125 conductivity meter with an Orion #011020 glass conductivity cell.

The enzyme leach selective extraction has once again been applied to b-horizon soil samples in this survey. This 
approach utilizes a phase-specific dissolution that liberates metals adsorbed onto the amorphous Mn-oxide coatings of 
individual mineral grains in the b-horizon. The leachate is analyzed using ICP-MS, and element concentrations are 
reported at parts per billion concentration levels. Because of the relatively thick cover of surficial deposits in this year’s 
study area and the successful application of this technique in year one of the project, this year b-horizon soils were 
only analysed using enzyme leach-ICP-MS technology.

An unique opportunity to assess the diamond potential for the Superior Province in Manitoba has been extended by 
cooperative efforts with MONOPROS Ltd. Eleven litre pails of till collected at each sampling site were concentrated, 
mineralogically picked and microprobed to provide mineral chemistry for classification purposes. Sample locations 
were withheld until release of the open file report to ensure equal opportunities for follow-up by all interested parties in 
the exploration community. This approach permitted diamond potential to be assessed in the 1997 survey area. Under 
normal circumstances the kimberlite indicator mineral survey would have been too costly for the Geological Services 
Branch to undertake.

In another beneficial cooperative arrangement with the Geological Survey of Canada, crown twig samples collected 
from black spruce trees were ashed in the GSC laboratories under the direct supervision of Dr. Colin Dunn. The 
opportunity to prepare vegetation geochemical samples with good control on ashing temperatures and contamination 
and to bracket analyses with vegetation geochemical standards prepared in these same laboratories, has resulted in 
the development of a well constrained vegetation geochemical database.

The element Hg was analysed in outcrop rock chip and humus samples as a specialty element. The analysis was 
undertaken at Activation Laboratories Ltd. (Ancaster, Ontario) using a flow injection mercury system designed by 
Perkin Elmer Ltd. Till was analyzed for Hg by cold vapour – atomic absorption spectrometry (AAS).

The interpretation of exploration geochemical data often relies upon the recognition of localized patterns of element 
variation. This approach to data interpretation is strongly recommended for the data presented from the 1997 
Operation Superior multimedia geochemical survey.

The format of this years (1998) multimedia geochemical survey report has been significantly modified from that 
produced in 1997. Data and preliminary interpretations for results from each of the sampling media are included in one 
binder. This was achieved by producing element-and media-specific percentile bubble plots for both the Edmund Lake 
and Sharpe Lake belts (NTS 53K) on the same page. This significantly reduces hardcopy volume. Finally, all text and 
graphical data is presented on CD-ROM for ease of computer applications. The design and construction of the CD-
ROM was undertaken by Paul Lenton of the Geological Services Branch.
METHODOLOGY

Multimedia geochemical samples were collected on approximately 1 km centres or as dictated by access to landing 
sites using a float equipped helicopter (Bell Jet Ranger 206B). The procedure at each site was to establish by way of 
hand augering, the location from which a till sample was to be collected. All other samples were collected in and 
around the immediate area of the till pit. Sample site locations were plotted on airphotos while viewing the sites from 
the helicopter subsequent to sample collection.

The specifics of sample collection, preparation and analyses, including data and derived products are described 
individually for each media type.
DATA DISPLAY

Geochemical data for all sample types are presented in table format with site identification and UTM coordinates. This 
same data is presented as delimited ASCII and EXCEL 4.0 files on CD-ROM in the back of this report. The variation in 
concentration of the various elements throughout the survey areas is presented as percentile intervals bubble plots 
produced using MAPINFO GIS software, digitized sample locations and analytical data. Percentile values represent 
the percentage of data points that fall below a certain analytical value; e.g. a 25th percentile value of 30 ppm Cu 
indicates that 25% of the data points have values for Cu that are less than 30 ppm. Likewise, at a 95th percentile value 
of 200 ppb Cu, only 5% of the data points would have values in excess of 200 ppm. Geochemical data from the 
Edmund Lake and Sharpe Lake greenstone belts is presented separately on the percentile bubble plots. This was 
done to preserve any geochemical characteristics in the datasets attributable to geological variations between the 
belts and variable metal assemblages in the mineralized zones.

This graphical display is a preliminary attempt to identify areas of high metal contents and thereby reduce the large 
areas surveyed to smaller areas for follow-up work. Although for any given area and sample media the number of 
samples may be low for the calculation of percentiles, the user can still quickly assess geochemical response by 
examining non-transformed geochemical data. Users can manipulate the geochemical data in the manner they feel 
appropriate to their needs by accessing the data on CD ROM. Elements consistently below the Lower Limit of 
Detection (LLD) have been excluded from the data tables and are not discussed further. Samples with concentrations 
below the LLD for any particular element are marked by a “<” symbol. For all plotting purposes a value of ½ of the LLD 
was substituted for a value below the LLD. For brevity and simplicity in the graphical display of geochemical data only 
total REE is plotted for rock, humus and vegetation data. Concentrations for individual REE are presented in the 
Appendices.

Users will note that the boundaries of the greenstone belts as well as simplified geology are presented on the 
percentile bubble plots. This was accomplished using a digital version of the 1:1 000 000 bedrock map of the province 
(Map 79-2) and the geological map of Corkery et. al., (1997a), respectively. Field sampling targets were located using 
the 1:250 000 Bedrock Geology Compilation Map Series maps for NTS 53K. UTM coordinates for sample sites are 
accurately derived from 1:50 000 topographic maps.

Mylar sample site location map overlays are provided to enable sample numbers to be derived by overlaying on the 
bubble plots.

BEDROCK GEOLOGY AND MINERAL DEPOSITS OF THE 1997 SURVEY AREAS

Multimedia geochemical and mineralogical surveys were conducted in the Edmund Lake and Sharpe Lake greenstone 
belts in 1997 (Figure 1). Simplified regional geology and mineral deposits in the survey area are presented in Figure 2. 
A sample site location map for these two belts is presented in Figure 3a and a mylar overlay in Figure 3b. The Edmund 
Lake belt in Manitoba extends from the Manitoba-Ontario border northwest to Edmund Lake for approximately 60 km. 
The Sharpe Lake belt trends east-west from the provincial boundary and was sampled as far west as the south shore 
of Webber Lake, a distance of approximately 90 km.

	Edmund Lake Belt

Previous geological mapping in the Edmund Lake belt was undertaken by Downie (1937) at a scale of 1:250 000 and a 
reconnaissance map of the Little Stull Lake area was produced by Corkery (1989). Corkery (1981) provided 
preliminary geological characteristics in the Little Stull Lake area. Most recently, geological mapping in the belt has 
been undertaken by Corkery (1996a, b) and Corkery et al., (1997a, b), as part of a larger geological initiative designed 
to critically assess mineral potential in Superior Province greenstone belts in Manitoba through lithologic, geochemical, 
structural and geochronological studies.

In the Edmund Lake – Margaret Lake area, the supracrustal belt forms a west-thinning, east-plunging homocline 
flanked by tonalite and granite terranes to the north and south. Lithologically, this portion of the belt is characterized by 
pillowed and massive basalt flows of the Hayes River Group (Downie, 1938). Gabbro and felsic dykes intrude the 
basalts. A 310o trending shear zone (“Wolf Bay Shear Zone” or WBSZ) transects the greenstone belt from the 
Manitoba-Ontario border. This deformation zone divides the belt into a northern and southern series of basalts. The 
northern edge of the Shear zone is marked by felsic and mafic volcaniclastic rocks, iron formation and sedimentary 
rocks (Corkery, 1996a) that were assigned to the Oxford Group by Downie (1938). Corkery (1996a) notes the 
presence of numerous rusty weathered zones in these units as well as within the Wolf Bay Shear Zone. A sample of 
silicified mafic tectonite from the north shore of Edmund Lake assayed 50 ppb Au (Corkery, 1996a). Preliminary map 
1996S-1 (Corkery, 1996b) at a scale of 1:20 000 presents the geological characteristics of this portion of the Edmund 
Lake belt and geological descriptions of individual lithologies are presented in Corkery (1996a).

A slight to moderate deflection of the WBSZ occurs approximately midway between the west end of Little Stull Lake 
and the east end of Margaret Lake. This deflection is characterized by a slight bend to a more westerly trend from its 
overall northwest-southeast attitude. This area is marked by a number of small lakes possibly occupying topographic 
depressions formed by the development of a dilational zone subsequent to right lateral movement along the WBSZ 
(Tim Corkery, pers. comm.).

Southeast of Edmund and Margaret Lakes, in the Little Stull Lake area, detailed mapping by Corkery et al., (1997a, b) 
has delineated 4 lithologically discrete structural panels. Each panel is characterized by a distinctive supracrustal 
assemblage and is in fault contact with adjacent panels. These panels, from south to north, comprise the following 
assemblages: 1) basalt and associated gabbro intrusions; 2) subaerial sandstone and conglomerate; 3) intermediate 
to felsic tuff, breccias, associated volcaniclastic and epiclastic rocks; and 4) basalt. Some panels can be traced 
northwestwards to the Edmund Lake area. Panels 1 and 4 are interpreted to represent Hayes River Group, Panel 2 is 
assigned to the sedimentary subgroup of the Oxford Lake Group and Panel 3 represents the volcanic subgroup of the 
Oxford Lake Group. A 77 m.y. time span between the deposition of the volcanic and sedimentary subgroups of the 
Oxford Lake Group is inferred on the basis of geochronological studies by Davis and Moore (1991) and Heaman (pers. 
comm., 1997 in Corkery et al., 1997a). The Little Stull Lake gold deposits that occur in this portion of the belt are 
associated with the Wolf Bay Shear Zone (WBSZ). This zone is developed within mafic volcanic flows and gabbroic 
synvolcanic intrusions of Panel 1. Details of these gold deposits are presented in a subsequent section. Recent 
geological mapping in the Little Stull Lake area has identified a quartz-feldspar porphyritic felsic intrusion at the 
northwest end of the lake. The western portion of this intrusion is altered to a sericite-pyrite assemblage. The 
metallogenetic significance of this late stage felsic intrusion as a heat engine and/or a metal source for the Little Stull 
Lake gold deposits is uncertain. Cutforth and Petak (1977) describe occurrences of barren sulphide mineralization in 
exposed areas of the belt.

Details of the individual lithologies and structures within the 4 lithostructural panels are available in Corkery et al., 
(1997a). These observations are depicted by Corkery et al., (1997b) in a 1:20 000 preliminary map of the area.

	Sharpe Lake Belt

The geological database for this greenstone belt is sparce. Downie (1936) mapped the Stull Lake area, including the 
Sharpe Lake belt, at a scale of 1 inch to 4 miles and the marginal notes that accompany these maps represent the 
bulk of the descriptive geological information presented here. Some details of the western portion of the belt from 
Webber Lake to Sharpe Lake were acquired from Marten (1973).

At the eastern most end of this belt in Manitoba, Downie (1936) mapped Hayes River Group felsic to mafic volcanic 
rocks with interbedded slate, quartzite and iron formation. Oxford Group sedimentary rocks, however, predominate 
over Hayes River Group volcanic rocks in this area. These sedimentary rocks include conglomerate, arkose, 
greywacke, slate, quartzite, chert and garnetiferous schist. Corkery et al., (1997) modified map 451A (Downie, 1936) 
by subdividing the Oxford Lake Group into a more northerly Volcanic Subgroup, represented by a west-thinning wedge 
of volcanic rocks that terminates just west of the Twin Lakes area, and a Sedimentary Subgroup.

The remainder of the belt, sampled in 1997, is described by Downie (1936) on Map 452A as predominantly Hayes 
River Group volcanic rocks. At Webber Lake, porphyritic rhyolite is described as the characteristic rock type. Locally 
the flows have been sheared to form “talcose sericite schists, well mineralized with pyrite”.

Marten (1973b) reported highly deformed supracrustal rocks in the Webber Lake area as consisting predominantly of 
fine grained schistose amphibolite and flattened pillow basalt. Strongly cleaved quartz porphyry and felsite units up to 
15m thick are interpreted as intrusions. Marten (1973) also notes ultramafic intrusions and four gabbroic dykes, up to 
80m thick, in the Webber Lake – Sharpe Lake portion of the belt.

Cutforth and Petak (1977) briefly describe the geology of this belt and note the presence of several small gossans in 
the nose of a fold developed in greywacke in the Sharpe Lake area. Graphitic and sulphidic iron formations, sparsely 
mineralized with chalcopyrite and sphalerite, are also mentioned from the Webber Lake area.


	Mineral Deposits

Significant mineralized zones in the 1997 survey area are represented by the Twin Lakes and Seeber River gold 
deposits in the Sharpe Lake belt and the Little Stull Lake gold deposits in the Edmund Lake belt (Fig. 3a). The 
following descriptions of these deposits are taken from Richardson and Ostry (1996), the most current literature 
available.

	Sharpe Lake Belt
	Twin Lakes Au Deposits

This gold deposit contains estimated preliminary reserves (“geological” reserves) of 2.45 million tonnes grading 2.5 
g/tonne in the “A” Zone and 472 000 tonnes grading 14.3 g/tonne in the “B” Zone.

Mineralization consists of sericitized and silicified felsic to intermediate, massive and fragmental volcanic rocks with 
pyrite and arsenopyrite. The gold zones are discontinuous high grade auriferous shoots encompassed by a large 
tonnage, low grade mineralized envelope. High grade intersections occur within massive, blue-grey quartz veins. B 
Zone high grade mineralization ranges from 6.73 to 24.16 g/tonne over 1.4 to 3.4 m. Low grade intersections range 
from 0.48 to 3.06 g/tonne over true widths of 2.0 to 34.0 m.

	Seeber River Au Deposit (C Zone)

This deposit is hosted by silicified and sericitized felsic volcanic rocks with arsenopyrite and pyrite and consists of a 
large, low grade mineralized zone (0.46 to 2.24 g/tonne over true widths of 4.0 to 52.0 m) with higher grade (5.9 to 
16.4 g/tonne over 3.0 to 6.7 m) intersections contained within it. The Seeber River C Zone contains 590 000 tonnes 
grading 9 g/tonne.

The Twin Lakes and Seeber River Au deposits occur within the east-west trending Twin Lakes-Monument Bay 
deformation zone that has been traced for 30 km. The known deposits have been delineated over a 3.5 km portion of 
this deformation zone at depths ranging from 20 to 460 m. Recent diamond drilling along the deformation zone 
approximately 1100 m west of the Seeber River deposit intersected 96 g/tonne Au over 2.9 m. This intersection 
strongly suggests that highly prospective nature of this deformation zone and its excellent residual exploration 
potential.

	Edmund Lake Belt
	Little Stull Lake Au Deposits

The Little Stull Lake gold deposits comprise 5 mineralized zones developed within an 8 km long structure that has 
been named the “Little Stull Break”. From southeast to northwest these are the Beaver Lodge, Rocky, Central, West 
and Otter Zones, (Fig. 4). Collectively, these zones comprise 750 000 tonnes grading 9.3 g/tonne.

The Little Stull Break forms part of the much larger Wolf Bay shear zone identified by Corkery (1996b). This shear 
zone is traced from Edmund Lake in the west, through Margaret Lake along the south shore of Little Stull Lake and on 
to the east end of Rapson Bay on Stull Lake (Figure 2). Mylonites and phylonites are developed within the zone as 
well as the interleaving of numerous rock types. Corkery (1996b) documents dextral kinematic indicators with strike 
slip movement and south side up based on shallow southeast to horizontal lineations. The structure appears to be 
developed at or near the contact between Hayes River Group mafic volcanic rocks and Oxford Lake Group 
sedimentary rocks.

Corkery (1997a) delineates the structural and alteration characteristics that are apparent in the area of the Little Stull 
Lake gold deposits. These include: 1) the deformation of mesogabbro by 310º trending mylonite; 2) significant 
albitization and silification of the sheared gabbro; 3) the filling of a closely spaced 340º-350º trending dilatational 
fracture cleavage, that is associated with the 310º shearing, by quartz and carbonate; and 4) sulphidization of the 
phylonites to produce variable amounts of pyrite.

These events are indicative of a protracted structural and alteration history responsible for suitable ground preparation 
for the formation of these deposits.


ACKNOWLEDGMENTS

Dan O’Donnell and Corey Taylor, Provincial Helicopters Limited (Lac du Bonnet), are acknowledged for their 
considerable skills in safely accessing sample sites for the 1997 sample season. Graham Carlyle and Cameron Toews 
are thanked for their enthusiastic support during the 1997 sampling season. Ron DiLabio and Harvey Thorleifson, 
Terrain Sciences, Geological Survey of Canada are thanked for their enthusiastic support and contributions to this 
project. The MAPINFO GIS system was provided by R. DiLabio and represents the main tool for data interpretation. 
Harvey Thorleifson is thanked for providing guidance with kimberlite mineral identification. Neill Brandson is thanked 
for logistical support during the field component of the project. Doug Berk, Rich Unruh, Gerry Benger, Vio Varga, 
Graham Carlyle and Cameron Toews are acknowledged for careful sample preparation. Don Snuggs is acknowledged 
for his analytical expertise and care with pH and conductivity measurements. We are grateful to Tim Corkery for 
discussions relating to recent geological observations in the Edmund Lake greenstone belt, particularly in the area of 
the Little Stull Lake gold deposits and along the Wolf Bay Shear Zone. Ifti Hosain provided valuable insights into the 
geophysical surveys conducted in the Edmund Lake and Sharpe Lake greenstone belts. Christine Kaszycki and Ric 
Syme are thanked for technical review of the manuscript. G. Conley is thanked for compiling the geochemical data and 
performing the statistical analysis. G. Matile produced all of the bubble plots used in this report and P. Lenton compiled 
all GIS data and assembled the CD-ROM version of the report. Kelly Proutt is thanked for typing the manuscript.


REFERENCES

Corkery, M.T.
1981:
Little Stull Lake area; in Manitoba Department of Energy and Mines, Mineral Resources Division, Report of Field 
Activities, 1981, p. 43-44.

Corkery, M.T.
1989:
Little Stull Lake area (Part of NTS 53K/10); Preliminary map 1989S-1, 1:20 000.

Corkery, M.T.
1996a:
Geology of the Edmund Lake area (53K/NE11); in Manitoba Energy and Mines, Minerals Division, Report of Activities, 
p. 11-13.

Corkery, M.T.
1996b:
Northeast Edmund Lake (53K/11NE); Manitoba Energy and Mines, Minerals Division, Preliminary Map 1996S-1, 1:20 
000.

Corkery, M.T., Skulski, T. and Whalen, J.B.
1997a:
Geology of the Little Stull Lake area (part of 53K/10); Manitoba Energy and Mines, Minerals Division, Report of 
Activities, 1997, p. 13-17.

Corkery, M.T., Skulski, T. and Whalen, J.B.
1997b:
Geology of the Little Stull Lake area (part of 53K/10); Manitoba Energy and Mines, Minerals Division, Preliminary Map 
1997S-1.

Cutforth, C. and Petak, H.W.
1977:
Webber-Sharpe Lakes and Edmund-Margeret Lakes greenstone belts (53L/8, 53K/5, 6, 10, 11, 14); in Manitoba 
Department of Mines, Resources and Environmental Management, Mineral Resources Division, Report of Field 
Activities, 1977, p. 159-161.

Davis, D.W. and Moore, M.
1991:
Geochronology in the Western Superior Province: summary report – May 1991; Internal Report, Jack Satterley 
Geochronology Laboratory, Royal Ontario Museum, Toronto, 7p.

Downie, D.L.
1936:
Stull Lake Sheet (East Half); Canada Department of Mines and Resources, Mines and Geology Branch, Map 451A.

Downie, D.L.
1938:
Stull Lake Sheet (West Half); Canada Department of Mines and Resources, Mines and Geology Branch, Map 452A.

Fedikow, M.A.F., Nielsen, E., Conley, G.G.
1997a:	
Operation Superior: 1996 Multimedia geochemical data from the Max Lake area (NTS 63I/8, 9 and 53L/5, 12); 
Manitoba Department of Energy and Mines, Mineral Resources Division, Open File Report OF97-1, 34p. and 1 disk.

Fedikow, M.A.F., Nielsen, E., Conley, G.G. and Matile, G.L.D.
1997b:
Operation Superior: Multimedia geochemical survey results from the Echimimish River, Carrot River and Munro Lake 
greenstone belts, northern Superior Province, Manitoba (NTS 53L and 63I); Manitoba Energy and Mines, Mineral 
Resources Division, Open File Report OF97-2, Part 1:Rock geochemical survey results (287p.), Part 2:Till 
geochemical survey results (105p.), Part 3:B-horizon soil geochemical survey results (432p.), Part 4:Humus 
geochemical survey results (188p.), Part 5:Vegetation geochemical survey results (437p.), Part 6:Kimberlite indicator 
mineral survey results (45p.),  2 diskettes.

Gold, T. and Soter, S.
1980:
The deep earth-gas hypothesis; Scientific American, vol. 242, p. 130-138.

Govett, G.J.S.
1976:
Detection of deeply buried and blind sulphide deposits by measurement of H+ and conductivity of closely spaced 
surface soil samples. J. Geochem. Explor., 6:359-382.

Govett, G.J.S., Dunlop, A.C. and Atherden, P.R.
1984:
Electrogeochemical techniques in deeply weathered terrain in Australia. J. Geochem. Explor., 21:311-331.

Hosain, I.
1997:
Summary of geophysical data from open assessment files of the Southern portion of the Gods Lake area, Manitoba; 
Manitoba Department of Energy and Mines, Mineral Resources Division, Open File Report OF97-4, 8p.

Malmqvist, L. and Kristiansson, K.
1984:
Experimental evidence for an ascending microflow of geogas in the ground; Earth and Planetary Science Letters, vol. 
70, p. 407-416.

Marten, B.E.
1973a:
Touchwood Lake-Gods Lake-Sharpe Lake Area (53L-6N, 7, 8, 9, 10; 53K-5W); Manitoba Department of Mines, 
Resources and Environmental Management, Mines Branch Geological Paper 2/73, p. 19-21.

Marten, B. and Elbers, F.J.
1973:
Manitoba Mines Branch Preliminary Map 1973 H-13, Murray Lake, 1” to ½ mile.

Matile, G.L.D. and Thorleifson, L.H.
1997:
Till geochemical and indicator mineral reconnaissance of northeastern Manitoba; Manitoba Department of Energy and 
Mines, Mineral Resources Division, Open File Report  OF97-3, 174p. 

Richardson, D.J. and Ostry, G. (revised by W. Weber and D. Fogwill)
1996:
Gold deposits of Manitoba; Manitoba Energy and Mines, Economic Geology Report ER86-1 (second edition).


Wang, X., Cheng, Z., Lu, Y., and Xie, ,X.
1997:
Nanoscale metals in Earthgas and mobile forms of metals in overburden in wide-spaced regional exploration for giant 
deposits in overburden terrains; J. Geochem. Explor., vol. 58, p. 63-72.

QUATERNARY GEOLOGY OF THE 1997 SURVEY AREAS
Stratigraphy

Large parts of the Edmund Lake-Sharpe Lake greenstone terrane is flat and monotonous with extensive wetlands and 
relatively few rock outcrops; exceptions being near the western ends of the belts around Edmund Lake and Sharpe 
Lake where rock outcrops are common. The sparse distribution of till samples (see till geochemistry maps) gives some 
appreciation of the wide distribution of fen and bog, which hindered sampling in the area. Wetland areas are 
particularly extensive in the areas east of Margaret Lake, west of Kistigan and Little Stull lakes and between 
Monument Bay and Twin Lakes where few till samples were collected. As a consequence of the flat terrane, 
observations on the Quaternary stratigraphy were limited to hand-dug pits.

The Quaternary stratigraphy as revealed from hand-dug pits consists of a single till sheet and an extensive blanket of 
fine grained glaciolacustrine silt and clay. Extensive wetlands, which are wide spread throughout the area, are 
underlain by fine textured glaciolacustrine sediments that also drape most of the surrounding hills, in places forming an 
impenetrable obstacle to sampling the underlying till from hand-dug pits. The extensive wetlands and the widespread 
glaciolacustrine sediments are the greatest impediments to till sampling from hand-dug pits in the area. 

The landscape of the area is dominated by the Sachigo Interlobate Moraine, which forms a large and very prominent 
south trending ridge along the east side of Little Stull Lake and Kistigan Lake. The 150 km long moraine formed 
between the eastern margin of the large ice lobe that occupied northeastern Manitoba and an equally large ice lobe 
situated in northwestern Ontario, during the latter part of the Wisconsinan. In the Kistigan-Little Stull Lakes area, the 
moraine appears to be composed of silt and fine sand giving rise to the sandy beaches and arcuate shorelines on the 
east side of those lakes. Further south in Ontario, the moraine is composed of sand and coarse gravel. The four 
eskers crossing the area are relatively narrow and are generally not an impediment to regional till sampling other than 
perhaps at the east end of Little Stull Lake, where a southeast trending esker crosses the greenstone belt before 
joining the Sachigo Moraine in Ontario. A southerly trending esker occurs at the east end of Edmund Lake and two 
south southwesterly trending eskers are found where the Red Sucker River enters Sharpe Lake and at Webber Lake.

The till is gray to beige, massive and sandy to silty similar to the till previously described in other parts of the northern 
Superior Province (Fedikow et al., 1997, Matile and Thorleifson 1997). In bedrock-dominated terrain the till forms thick 
accumulations of lee-side till, down ice from bedrock obstructions, but also commonly occurs as drumlins or drumlinoid 
ridges tens of metres high and several kilometres long. A large proportion of the till is allochthonous having been 
derived from the Paleozoic carbonate terrain of the Hudson Bay Lowland. Paleozoic carbonate, Proterozoic Omarolluk 
greywacke and iron formation erratics derived from the Hudson Bay Lowland are common constituents of the till 
throughout the area. Matile and Thorleifson (1997) indicate the till matrix (<63 micron) in this area is composed of 
approximately 20% calcite and 20 % dolomite whereas the pebble fraction (8-16 mm) is about 45-69 % distantly 
traveled carbonate. Other erratics including distinctive granites, rhyolites, dacites, a variety of arkoses and 
conglomerates and quartzite’s from various sources in northern Manitoba, Keewatin and eastern Hudson Bay further 
testify to the allochthonous character of the till.

Ice Flow Direction

Glacial striae recorded at twelve sites in the Edmund Lake belt ranged between 176° and 198° whereas striae at 
fourteen sites in the Sharpe Lake belt ranged between 179° and 227°. The more southerly and south southeasterly 
striae were found at the eastern end of both belts. Towards the west the orientation gradually changes to become 
more southwesterly. Older striae towards 250° and 280° were recorded at two sites and T. Corkery (pers. comm. 
1997) observed older striae trending 225° cut by younger striae at 176° in Little Stull Lake. The older striae testify to an 
earlier westerly ice flow, which is believed to have had little impact on the observed glacial dispersal pattern recorded 
by the dominant striae direction and till composition.

The orientation of drumlins and drumlinoid ridges is similar to the orientations recorded by the glacial striae. Drumlins 
in the Margaret Lake-Little Stull Lake-Monument Bay area trend towards 175°. At the west end of the belts, in the 
Barclay Lake-Webber Lake area, drumlins are orientated towards 200° and south of the west end of Edmund Lake 
towards 195°. In the area near the center of the belts, such as immediately west of Makataysip Lake, drumlins are 
orientated towards 185°.



ROCK GEOCHEMICAL SURVEY
Sample Collection, Preparation and Analysis

Outcrop rock chip samples were collected from the Edmund Lake and Sharpe Lake greenstone belts after moss mats 
and soil were removed from the outcrop. A total of 77 samples were collected from the Edmund Lake belt and 49 from 
the Sharpe Lake belt. A representative sample consisted of 3-4 fist-sized chips. These chips were jaw crushed to 
maximum 5 mm fragments and powdered in a tungsten carbide swing mill. The powders were homogenized by rolling 
and then split and placed into vials each weighing approximately 55 grams. Vials were then submitted for INA and ICP-
AES analyses at Activation Laboratories Ltd. The ICP-AES analyses are based upon a four acid total digestion. Hg 
was analyzed using a flow injection mercury system developed by Perkin-Elmer Ltd. Hydrogen ion (H+) and specific 
conductance were analysed in the Geological Services Branch laboratory. Descriptions of outcrop rock chip samples 
are given in Appendix 1. Geochemical data is presented in Appendices 2 (ICP-AES, H+, K and Hg) and 5 (INAA); 
geochemical data for sites where more than one sample was collected is presented in Appendices 3 (ICP-AES, H+, K 
and Hg) and 6 (INAA). Percentile bubble plots are in Appendices 4 (ICP-AES, H+, K and Hg) and 7 (INAA). In 
Appendix I the user will notice there are occasionally two outcrop rock chip samples collected from a single site. In this 
case the sample with the highest analysis of a particular element was used for plotting purposes.

Format

Results are presented as a descriptive narrative of geochemical flux in both the Edmund Lake and Sharpe Lake 
greenstone belts. This narrative takes the form of relating the variation in concentration of individual elements to 
geological features such as rock types or structures. In a subsequent section entitled “synthesis” a detailed discussion 
and summary of element variations integrating specific geophysical signatures, mineral deposits and geological 
characteristics, is presented.

Elements are grouped and discussed in turn according to their analytical technique. Accordingly, the descriptions 
proceed from Hg (FIMS) to INA to ICP-AES and finally H+ and specific conductance results.

Results
	Flow Injection Mercury System (FIMS)

Hg:	The highest Hg values occur in two areas in the Edmund Lake belt. These are:
	(i)	northwest of Little Stull Lake in association with an altered high level quartz-feldspar-porphyry, and;
	(ii)	the highest value of the 1997 survey 531 ppb Hg was obtained near the Manitoba-Ontario provincial boundary 
in the Edmund Lake belt; a third site of elevated Hg occurs north of the west end of Sharpe lake where 99th and 
100th percentiles of 54-83 ppb occur.

	Instrumental Neutron Activation (INA)

Au:	The host rocks to the Little Stull Lake Au deposits are marked by 220 ppb Au and a cluster of 90-99th percentiles 
south and east to the Manitoba-Ontario boundary. Elevated 90-98th percentile Au values also occur on the west 
shore of Edmund Lake and on islands in the centre of the lake. These high values are associated with ultramafic 
sills and dykes deformed by the Wolf Bay Shear Zone (WBSZ). Multiple 90th and 95th percentiles occur in samples 
from the periphery of a felsic intrusion at Margaret Lake.

	Au is less elevated in samples collected from the Sharpe Lake belt with 40 ppb Au representing the 100th 
percentile.

The highest Au contents occur near the southern margin of the belt south of Makataysip Lake (40 ppb) and Twin 
Lakes (22-27 ppb).

As:	The variation in concentration of As essentially mimics that of Au in the Edmund Lake belt. The area of the Little 
Stull Lake gold deposits is marked by a 3800 ppm response (100th percentile); a “rim” of up to 27 ppm As (95th 
percentile) is developed around the Margaret Lake intrusion. A 200 ppm As anomaly (98th percentile) occurs at the 
Manitoba-Ontario border near the confluence of the Edmund Lake and Sharpe Lake belts.

	In the Sharpe Lake belt the 100th percentile for As (2000 ppm) occurs southwest of Makataysip Lake near the 
southern margin of the belt. Additional anomalies occur at Monument Bay (99th percentile, 1500 ppm) and south of 
Twin Lakes near the southern margin of the belt (98th percentile, 200 ppm).

Ba:	The highest Ba responses in the Edmund Lake belt occur (i) at the deflection point of the WBSZ (100th percentile, 
2600 ppm) (ii) southeast of the Little Stull Lake gold deposits along the WBSZ (99th percentile, 1200 ppm), (iii) 
southeast of Ken Bay on Little Stull Lake near the Manitoba-Ontario border (95th percentile, 770 ppm) and (iv) at 
the southeast end of the Margaret Lake intrusion (95th to 98th percentiles, 770-1000 ppm).

	Both the Monument Bay area (100th percentile, 930 ppm Ba) and the southern portion of the Twin Lakes area (99th 
percentile, 890 ppm Ba) exhibit elevated Ba contents in the Sharpe Lake belt. A 98th percentile response of 800 
ppm Ba occurs south of Makataysip Lake.

Br:	The area southeast of Little Stull Lake in the Edmund Lake belt is marked by a cluster of relatively low contrast Br 
responses (98th-100th percentiles, up to 6.7 ppm).

	In the Sharpe Lake belt a single sample response of 19 ppm Br (100th percentile) occurs due south of Makataysip 
Lake near the southern margin of the belt. The northwest shore of Sharpe Lake and the north shore of the west 
end of Sharpe Lake are both marked by 2 sample Br responses of between 8.9 and 12 ppm.

Ca:	Generally suppressed responses are observed throughout both greenstone belts. In the Edmund Lake belt the 
highest responses are associated with the Margaret Lake intrusion (up to 13%).

	A range of 8-15% Ca is documented from samples collected along the north shore of Sharpe Lake and west 
towards Webber Lake.

Co:	A cluster of 90th-99th percentile values are associated with the Margaret Lake intrusion in the Edmund Lake belt. 
Two samples east and south of the Little Stull Lake gold deposits are marked by the 98th percentile (75 ppm) for 
Co. The 100th percentile (98 ppm) occurs at the Manitoba-Ontario provincial border near the confluence of the two 
belts.

	In the Sharpe Lake belt the highest Co responses are observed in the Twin Lakes area (100th percentile, 85 ppm), 
62-66 ppm (90th-98th percentile) at Makataysip Lake and 98th percentile responses on the north shore of the east 
end of Sharpe Lake.

Cr:	The range 780-1100 ppm Cr (99th and 100th percentiles) were obtained from samples collected in the central 
portion of the WBSZ at the deflection point of the trend of this structure. Two 95th percentile (360 ppm) responses 
are observed on the south shore of Kistigan Lake and near the Manitoba-Ontario border at the confluence of both 
belts. The highest response of 1200 ppm (100th percentile) occurs south of Makataysip Lake near the Southern 
margin of the belt in an area of no apparent anomalous geophysical response.

Cs:	In the Edmund Lake belt the 100th percentile response of 10 ppm occurs west of Little Stull Lake. A cluster of 90th-
98th percentiles (2-4 ppm) trend south from Little Stull Lake to the Manitoba-Ontario provincial border.

	The Sharpe Lake belt is marked by 2 main areas of elevated Cs response. These occur south of Twin Lakes (22 
ppm; 100th percentile) and west along the southern margin of the belt to Makataysip Lake (3-6 ppm).

Fe:	In the Edmund Lake belt the highest Fe contents occur in 3 samples of near solid to solid magnetite layers 
collected from the west-end of a small lake just east of Margaret Lake. The 100th percentile for Fe (26.40%) is 
obtained from this site. Both 95th and 98th percentiles (12.5% and 21.2%, respectively) for Fe occur southeast of 
Little Stull Lake, near the Manitoba-Ontario border.

	In the Sharpe Lake belt the Makataysip Lake area is marked by the 100th percentile Fe response (13.1%). The 
area of the chip sample is marked by a circular 6700 nT aeromagnetic anomaly. A 99th percentile response 
(12.6%) occurs west of Makataysip Lake, 98th (10.0%) and 95th (9.40%) percentiles occur west of Monument Bay 
and along the south margin of the belt south of Twin Lakes, respectively.

Hf:	Moderate to low contrast Hf responses (5-7 ppm) occur in the area of the Little Stull Lake gold deposits as well as 
to the north and west of the mineralization.

	The 100th percentile (12 ppm) Hf response in the Sharpe Lake belt occurs in the southern portion of the Twin 
Lakes area. A string of 3-5 ppm Hf responses occur west of Makataysip Lake to Sharpe Lake.

Mo:	In the Edmund Lake belt elevated Mo responses are spatially associated with the WBSZ; the 100th percentile of 41 
ppm Mo, however, occurs at or near the northeast portion of the Margaret Lake intrusion. Elsewhere along the 
WBSZ (including the WBSZ deflection), values of up to 11 ppm Mo (98th percentile) are obtained.

	The Sharpe Lake belt is characterized by very low contrast Mo responses. The Monument Bay and Twin Lakes 
areas, as well as one-site in Sharpe Lake area marked by the 98th percentile Mo response (6 ppm).

Na:	Areally extensive zones of significant Na depletion were not detected in either the Edmund Lake or Sharpe Lake 
belts. The 100th percentile of 5.29% Na occurs near the east side of Edmund Lake in a felsic (albitite?) dyke within 
the WBSZ.

	The 100th percentile Na response (4.48%) in the Sharpe Lake belt occurs on the north central shore of Sharpe 
Lake.

Ni:	In the Edmund Lake belt elevated Ni responses (99th percentile, 170 ppm) occur on an island in central Edmund 
Lake reflecting the presence of an ultramafic sill. The east end of the Margaret Lake intrusion is characterized by 
90th-98th percentile responses (93-140 ppm). The 100th percentile (190 ppm) occurs at the WBSZ deflection.

	The Sharpe Lake belt is characterized by higher Ni responses. The 100th percentile (360 ppm) occurs south of 
Makataysip Lake; a 98th percentile response (200 ppm) occurs east of the Makataysip Lake aeromagnetic 
anomaly. Both responses are situated near the southern margin of the belt. The north shore of the east end of 
Sharpe Lake is marked by a string of 90-95th percentile responses (140-180 ppm).

Rb:	In the Edmund Lake belt a cluster of elevated Rb responses occur in the general area of the west end of Little Stull 
Lake which includes the 100th percentile of 89 ppm. Significant responses occur at the east end of the Margaret 
Lake intrusion (99th percentile, 69 ppm) and on the east side of Edmund Lake (95th-98th percentiles, 53 and 55 
ppm, respectively).

	The highest Rb contents in the Sharpe Lake belt occur on the north shore of the west end of Sharpe Lake (100th 
percentile, 170 ppm).

	The 99th percentile (160 ppm) occurs at the south end of Twin Lakes. A string of 90th-98th percentile responses 
(100-120 ppm) occurs south and west of Makataysip Lake along the southern margin of the belt.

Sb:	The distribution of elevated Sb in the Edmund Lake belt is observed to be spatially related to the WBSZ. This 
includes the 100th percentile (45 ppm) obtained from the host rocks to the Little Stull Lake Au deposits. A 98th 
percentile response (4.4 ppm) occurs northeast of the mineralization in association with an altered felsic intrusion. 
Two other separate clusters of 90th-95th percentile (0.9-1.5 ppm) responses are observed at the WBSZ deflection 
and further to the northwest near the east end of the Margaret Lake intrusion.

	The highest Sb response of the survey was (63 ppm) was recorded in a sample collected on the north shore of the 
west end of Sharpe Lake. A 98th percentile response of 10 ppm occurs south of Makataysip Lake near the 
southern margin of the belt. A 95th percentile (7.40 ppm) occurs on the north shore of Monument Bay.

Sc:	The highest Sc contents in the Edmund Lake belt are observed southeast of Little Stull Lake near the Manitoba-
Ontario border. These are 99th and 100th percentiles (48 and 57 ppm, respectively). A 95th percentile (45 ppm) 
occurs west of Little Stull Lake along the WBSZ.

	In the Sharpe Lake belt the 100th percentile response of 49 ppm occurs on the southwest shore of Makataysip 
Lake in association with a 6700 nT aeromagnetic response. Two areas of 98th percentile responses (41 ppm) 
occur near the central portion and west end of Sharpe Lake.

Ta:	Low contrast Ta responses are apparent from both greenstone belts surveyed in 1997. Values of >2 ppm occur at 
and in the general are of the Little Stull Lake gold deposits as well as near the south shore of Margaret Lake (100th 
percentile, 2.5 ppm).

	The 100th percentile of 2.3 ppm Ta in the Sharpe Lake belt occurs on the south end of Twin Lakes.

Th:	Three sites of elevated Th are documented from the Edmund Lake belt. These are the Little Stull Lake area, 
including the gold mineralized zone (98th percentile, 16 ppm), the WBSZ deflection (98th and 99th percentiles, 16 
and 17 ppm respectively) and the east end of Margaret Lake where the 100th percentile response (22 ppm) is 
recorded.

	Significant Th responses from the Sharpe Lake belt include the north and south areas of Monument Bay (98th and 
95th percentiles of 17 and 10 ppm respectively), the south end of Twin Lakes (100th percentile, 26 ppm) and the 
area southwest of Makataysip Lake (99th percentile, 22 ppm) along the south margin of the belt.

U:	The U response is similar to that of Th. In the Edmund Lake belt the 100th percentile response (6.9 ppm) occurs 
near the east end of Margaret Lake and the Margaret Lake intrusion. The WBSZ deflection is marked by 95-99th 
percentile U responses (2.3-3.4 ppm) and the Little Stull Lake gold deposits are characterized by 90th-98th 
percentiles for U (1.8-3.0 ppm).

	Four sites of elevated U are apparent from the Sharpe Lake belt survey. The 100th percentile of 6.7 ppm U occurs 
south of Makataysip Lake near the south margin of the belt. The Twin Lakes and Monument Bay areas are 
marked by 90th-98th percentle (2.6-5.4 ppm) and 90th-95th percentiles (2.6-4.3 ppm), respectively. A 99th percentile 
(5.6 ppm) was obtained from a sample on the north shore of the west end of Sharpe Lake.

W:	In the Edmund Lake belt the 100th percentile (900 ppm) for W occurs at the east end of the Margaret Lake 
intrusion. A 99th percentile (800 ppm) occurs south of the intrusion. The area of the Little Stull lake gold deposits is 
marked by 98th (730 ppm) and 95th (600 ppm) percentile responses. An island in central Edmund Lake is marked 
by a 98th percentile response.

	The southern end of Twin Lakes in the Sharpe Lake belt contains the 100th percentile W response (730 ppm) with 
other elevated W in the area southwest of Makataysip Lake (98th percentile, 730 ppm) and along the north shore of 
the east end of Sharpe Lake (90-98th percentiles, 360-730 ppm).

Zn:	The 100th percentile response (391 ppm) for Zn in the Edmund Lake belt occurs southeast of Little Stull Lake. The 
host rocks to gold mineralization at Little Stull Lake have a 99th percentile response of 372 ppm. The west end of 
Margaret Lake and an island in central Edmund Lake are both characterized by 98th percentile (280 ppm) 
responses.

	The Sharpe Lake belt contains elevated Zn concentrations at Makataysip Lake (98th percentile, 230 ppm) and 5 
km west of Makataysip Lake (100th percentile, 276 ppm). South of Twin Lakes 90th to 95th percentile responses 
(193-209 ppm) were obtained from an area close to the southern margin of the belt. A 98th percentile of 230 ppm 
Zn occurs in central Sharpe Lake.

REE:

	The rare earth element response is presented as the “total” or summation of individual REE for purposes of 
simplicity and brevity in this report. Individual REE analyses are presented in the Appendices. In the Edmund Lake 
belt the highest total REE are obtained from 2 sites (100th and 99th percentiles, 351.4 and 334.2 ppm, respectively) 
at the WBSZ deflection. Additional sites of elevated REE occur in a semi-circular arc extending from the south 
shore of Kistigan Lake (98th percentile, 300.7 ppm) to the north and west shores of Little Stull Lake (both 95th 
percentiles, 237 ppm) to the area east and southeast of Little Stull Lake (95th and 98th percentiles, 237 and 300.7 
ppm, respectively). The host rocks to the Little Stull Lake Au deposits are characterized by 90th percentile 
responses (141 ppm).

	In the Sharpe Lake belt most elevated responses occur east of Sharpe Lake to Monument Bay. The 100th 
percentile occurs in the southern portion of Twin Lakes (529.6 ppm) with 95th and 98th percentile responses (143.7 
and 402.8 ppm, respectively) at Monument Bay and 98th percentiles southwest of Makataysip Lake near the 
southern margin of the belt.

	Inductively Coupled Plasma-Atomic Emission
	Spectrometry (ICP-AES)

Mo:	Mo concentrations in the Edmund Lake belt are generally low with a single sample 100th percentile response of 54 
ppm occurring on the east end of Margaret Lake and adjacent to the Margaret Lake intrusion. A 99th percentile (7 
ppm) occurs at the WBSZ deflection. The area of the Little Stull Lake gold deposits is marked by 95th and 98th 
percentile responses (3 and 5 ppm, respectively). This same signature occurs southeast of Ken Bay, Little Stull 
Lake.

	Four sites along the Sharpe Lake belt contain 2 ppm Mo.

These are the Monument Bay area, Makataysip Lake, east and west Sharpe Lake. These values are not 
considered to be significant.

Cu:	Three main areas of elevated Cu contents are present along the Edmund Lake belt. The 100th percentile of 411 
ppm occurs south of the east end of the Margaret Lake intrusion. West of the Little Stull Lake gold deposits is a 
single site 99th percentile response (288 ppm) and southeast of Ken Bay is a cluster of 6 sites of 95th and 98th 
percentiles (243 and 276 ppm, respectively).

	The Cu responses in the Sharpe Lake belt are highest from a single site on the north shore of Sharpe Lake (100th 
percentile, 231 ppm) with lesser responses midway between Sharpe and Makataysip Lake (98th percentile, 276 
ppm) and south of Twin Lakes near the southern margin of the belts (90th – 99th percentiles, 176-288 ppm).

Zn:	The 100th percentile Zn response in the Edmund Lake belt (447 ppm) is from the site of the Little Stull Lake gold 
deposits. The 99th percentile response (429 ppm) occurs southeast of Ken Bay. A 98th percentile (294 ppm) 
response occurs in near solid to solid, magnetite-rich iron formation exposed in outcrop at the west end of 
Margaret Lake.

	Zn response in the outcrop chip samples collected from the Sharpe Lake belt is relatively subdued. The 100th 
percentile of 145 ppm occurs midway between Sharpe and Makataysip Lakes. The 99th percentile (121 ppm) 
occurs on the southwest shore of Makataysip Lake in association with a 6000 nT aeromagnetic response.

Ag:	Ag values in both the Edmund Lake and Sharpe Lake belts are low. In the Edmund Lake belt the maximum value 
of 1.9 ppm is obtained from the area of the WBSZ deflection. A cluster of values between 0.5-0.9 ppm occur in 
spatial association with the Margaret Lake intrusion. There appears to be a relatively strong association between 
detectable Ag in rock samples and proximity to the WBSZ. This is particularly well developed along the northwest 
portion of the WBSZ. The maximum value of 1.0 ppm Ag in the Sharpe Lake belt occurs on the north shore of the 
west end of Sharpe Lake.

Pb:	The 100th (55 ppm), 99th (30 ppm) and 95th (15 ppm) percentile Pb responses at the Little Stull Lake gold deposit, 
including the areas on the west and north shores of the lake, represent the highest and probably most significant 
responses in the Edmund Lake belt. A 98th percentile response of 27 ppm occurs at the east end of the Margaret 
Lake intrusion.

	Significant Pb signatures in outcrop chip samples from the Sharpe Lake belt are restricted to the central portion of 
Sharpe Lake (100th percentile, 64 ppm), the west end of Sharpe Lake (98th percentile, 41 ppm) and the southern 
portion of the Twin Lakes area (99th percentile, 30 ppm). Lesser Pb responses occur at north and south Monument 
Bay and southwest of Makataysip Lake along the southern margin of the belt.

Ni:	The 100th percentile (342 ppm) in the Edmund Lake belt occurs at the WBSZ deflection with a subsidiary cluster of 
95th and 98th percentile responses (173 and 191 ppm, respectively) occurring near the east end of the Margaret 
Lake intrusion. A 99th percentile response (203 ppm) occurs on the north shore of Rorke Lake and a 98th percentile 
(191 ppm) response is situated at the confluence of the Edmund Lake and Sharpe Lake belts near the Manitoba-
Ontario border.

	In the Sharpe Lake belt the 100th percentile Ni response (386 ppm) occurs south of Makataysip Lake with a 99th 
percentile site (192 ppm) eastwards along the southern margin of the belt. Central Sharpe Lake is the site of a 98th 
percentile response (188 ppm).

Mn:	Significant Mn responses are limited to the west end of Margaret Lake where the 100th percentile (19743 ppm) is 
associated with exposed near solid to solid, magnetic-rich iron formation. A cluster of 95th to 99th percentile 
responses (4155 to 9675 ppm) occur between the WBSZ east of Little Stull Lake and the southern margin of the 
belt near the Manitoba-Ontario border.

	Mn response in the Sharpe Lake belt is somewhat subdued in comparison to the Edmund Lake belt. The 100th 
percentile (3476 ppm) occurs south of Twin Lakes near the southern margin of the belt. The 95th to 99th percentile 
responses occur at single sites between Makataysip Lake and eastern Sharpe Lake. The Mn contents along this 
portion of the belt vary from 2090 to 2929 ppm.

Sr:	Significant Sr responses occur at the site of the Little Stull Lake gold deposits (100th percentile, 1386 ppm) and on 
the north shore (98th percentile, 1059 ppm) and west shore (95th percentile, 1014 ppm) of Little Stull Lake. A 
second zone of elevated Sr occurs at the deflection of the WBSZ (99th percentile, 1088 ppm). A 98th percentile 
response (1059 ppm) occurs on the north shore of Margaret Lake.

	In the Edmund Lake belt both the 100th and 99th percentile responses are centered on the Monument Bay area 
(847 and 642 ppm, respectively). A 98th percentile site (608 ppm) occurs southwest of the south end of Twin Lake.

Bi:	Bi responses in outcrop chip samples are of low contrast in both the Edmund Lake and Sharpe Lake belts. The 
100th percentile in the Edmund Lake belt (8 ppm) occurs near the northeast corner of the Margaret Lake intrusion 
and the 99th percentile (7 ppm) is situated at the west end of Little Stull Lake in association with an altered felsic 
intrusion. A 98th percentile response is documented from an area south of the Margaret Lake intrusion and also 
from the area of the confluence of both greenstone belts near the Manitoba-Ontario border.

	The highest Bi response in the Sharpe Lake belt (8 ppm) is situated southwest of Makataysip Lake in association 
with a 98th percentile response of 6 ppm. A second value of 6 ppm is located northwest of Monument Bay.

V:	Three zones of elevated V occur along the Edmund Lake belt. These are (i) north shore of Margaret Lake (100th 
percentile, 419 ppm), (ii) a cluster of 99th and 98th percentile responses centered on the deflection of the WBSZ, 
and (iii) 95th and 98th percentiles near the confluence of the belts at the Manitoba-Ontario border.

	In the Sharpe Lake belt the 100th percentile of 527 ppm occurs on the southwest shore of Makataysip Lake in 
association with a 6700 nT aeromagnetic response. The north shore of the west end of Sharpe Lake is 
characterized by two adjacent 98th percentile (298 ppm) sites.

Ca:	The 100th and 99th percentile responses on the Edmund Lake belt occur to the north (14.21%) and south (13.97%), 
respectively of the Margaret Lake intrusion. The area southeast of the deflection of the WBSZ is marked by a 98th 
percentile (13.34%) response.

	In the Sharpe Lake belt the 100% percentile (16.55%) response occurs south of Webber Lake. A 98th percentile 
response (14.14%) is documented from the east end of Sharpe Lake.

P:	Phospherus responses in the Edmund Lake belt are somewhat scattered, however, two main areas of enrichment 
are present. The 100th percentile response (0.55%) occurs on the south shore of Kistigan Lake with the 99th 
(0.211%) and 98th (0.195%) percentile sites clustered at the deflection of the WBSZ. Scattered 95th (0.155%) and 
98th percentile responses occur southeast from Little Stull Lake to the Manitoba-Ontario border.

	The most significant P responses are associated with the Twin Lakes and Monument Bay areas in the Sharpe 
Lake belt. The 100th percentile (0.19%) occurs in the southern area of Twin Lakes, 95th and 98th percentile (0.105 
and 0.165%, respectively) occur at Monument Bay.

Mg:	A single area of Mg enrichment is recognized in the Edmund Lake belt. The 100th, 99th and 98th percentile (8.01, 
6.13 and 5.47%, respectively) responses are all situated on or near the deflection of the WBSZ.

	The 100th percentile Mg response (9.28%) in the Sharpe Lake belt occurs south of Makataysip Lake with two 98th 
percentile sites (5.62%) occurring along the northern shore of the western half of Sharpe Lake.

Ti:	Ti enrichments are generally moderate to low contrast for both greenstone belts. In the Edmund Lake belt the 
100th percentile (1.23%) occurs on the north side of Margaret Lake. The deflection of the WBSZ is marked by 99th 
(1.02%), 98th (0.89%) and 95th (0.76%) percentile responses. West of Little Stull Lake is a 98th percentile response 
of 0.89% Ti.

	In the Sharpe Lake belt the 100% percentile response of 1.34% Ti occurs on the southwest shore of Makataysip 
Lake in association with a circular 6700 nT aeromagnetic anomaly. A 98th percentile response (1.12% Ti) occurs 
west of Makataysip Lake and south of Twin Lakes near the southern margin of the belt.

Al:	Elevated Al in the Edmund Lake belt occurs at the confluence of the two greenstone belts near the Manitoba-
Ontario border where 100th percentile (11.36%) and 98th percentile (9.48%) responses are documented. The area 
north and east of the Margaret Lake intrusion is characterized by 99th percentile (10.62%) and 98th percentile 
(9.48%) responses.

	The Monument Bay (100th percentile, 10.16%) and Twin Lakes area (99th and 98th percentiles, 9.84 and 9.11% 
respectively) represent sites with elevated Al contents in the Sharpe Lake belt.

K:	The site significant K enrichment in the Edmund Lake belt occurs in the area of the gold mineralization and 
associated altered felsic intrusion at Little Stull Lake. K contents range from 2.74% (100th percentile) to 1.42% (95th 
percentile). A second zone of elevated K occurs on the east shore of Edmund Lake where 98th percentile (2.26%) 
responses are documented. Both zones of K enrichment occur along the WBSZ.

	Three sites of K enrichment occur in the Sharpe Lake belt and include the 100th percentile (4.97%) site south of 
Makataysip Lake, the southern end of Twin Lakes (98th percentile, 3.98%) and the northern area of Monument Bay 
(98th percentile, 3.98%).

Y:	The main zone of Y enrichment in the Edmund Lake belt occurs along the “central” segment of the WBSZ 
extending from the west end of Little Stull Lake to the point of deflection of the WBSZ. Within this zone 100th (80 
ppm), 99th (60 ppm) and 98th (50 ppm) percentile responses for Y are documented. A 95th percentile response (41 
ppm) also occurs on the north shore of Margaret Lake.

	In the Sharpe Lake belt, Y is elevated on the west shore of Makataysip Lake (99th percentile, 46 ppm) in 
association with a 6700 nT aeromagnetic signature and west of Makataysip Lake (100th percentile, 86 ppm).

	Hydrogen Ion (H+)

H+:	Hydrogen ion, the corrected form of pH, is significantly elevated at two sites along the Edmund Lake belt. The 
100% percentile (55.5 ppb) occurs at the west end of Margaret Lake where near solid to solid, magnetite-rich iron 
formation was sampled. The second site occurs near the confluence of both the greenstone belts at the Manitoba-
Ontario border.

	No significant H+ responses are noted from the Sharpe Lake belt.

	Specific Conductance (Water-Extractable Metal)

K:	The 100th and 99th percentile responses (154.57 and 86.66 mhos cm-1, respectively) for K are documented from 
the west end of Margaret Lake where magnetite-rich iron formations were sampled. The area of the Little Stull 
Lake gold deposits and the area of belt confluence near the Manitoba-Ontario border represent sites of 98th 
percentile (60.35 mhos m-1) responses. In the Sharpe Lake belt the 100th percentile (44.81 mhos cm-1) occurs 
south of Makataysip Lake near the southern margin of the belt. The areas south of Twin Lakes near the southern 
margin of the belt and the southern Monument Bay area are both characterized by 98th percentile responses 
(35.50 mhos cm-1).

Synthesis

There is a significant rock geochemical and geophysical relief in the 1997 multimedia geochemical survey area that 
can be attributed to the presence of known mineral deposits and geological features. Each of these features is 
reviewed in relation to their individual rock geochemical responses.

	Edmund Lake Belt

The Little Stull Lake area is marked by the presence of the Little Stull Lake gold deposits that occur within a 
deformational zone called the Wolf Bay Shear Zone (WBSZ). Five gold mineralized zones occur within an 8 km section 
of the WBSZ, locally referred to as the Little Stull Lake break. Rocks in the area have been mylonitized, silicified and 
albitized as well as sulphidized and crosscut by quartz and carbonate veinlets. The area is contained in its entirety by 
a gravity high and is also marked by linear and circular shaped aeromagnetic anomalies with associated adjacent or 
coincident strong to medium airborne EM conductors.

Outcrop rock chip geochemical data reflects the presence of the gold mineralization on the west shore of Little Stull 
Lake. Host rocks to the mineralization are characterized by 100th percentile responses for Au (220 ppb), As (3800 
ppm), Sb (45 ppm), Pb (55 ppm), K (2.74%), Sr (1386 ppm) and Y (80 ppm). Other significant responses include 99th 
percentiles for Cu (288 ppm), Hg (80 ppb), Bi (7 ppm) and Zn (447 ppm by ICP-AES, 372 ppm by INAA) as well as 98th 
percentiles for Co (75 ppm), Mo (5 ppm by ICP-AES, 11 ppm by INAA), Ba (1000 ppm), U (3 ppm), Th (16 ppm) and 
specific conductance (60.35 mhos cm-1).

These metal assemblages are typical of mineralization-related alteration in the immediate area of the deposit. Sample 
97R-131 collected just west of the northwest end of Little Stull Lake signifies the style of mineralization observed in 
outcrop. It comprises disseminated and laminae of pyrite, pyrrhotite and minor chalcopyrite in an altered, sericitic fine 
to medium grained basalt or gabbro.

A persistent multi-element geochemical signature was observed southeast of Little Stull Lake to the Manitoba-Ontario 
provincial border. In this general area two east-west trending moderate strength airborne EM conductors coincide with 
a 1400 nT aeromagnetic response. Samples collected in this general area are characterized by 100th percentile 
responses for Zn (429 ppm by ICP-AES, 391 ppm by INAA), Co (98 ppm), Hg (531 ppb), Br (6.7 ppm), Sc (57 ppm) 
and Al (11.36%). Ninety-ninth percentiles for H+ (31 ppb) and specific conductance (60.35 mhos cm-1) as well as 98th 
percentiles for Au (150 ppb), As (200 ppm), Sb (4.4 ppm), Cu (276 ppm), Bi (6 ppm), Ni (191 ppm), Fe (21.2%), V (357 
ppm) and Cs (4 ppm). The highest responses from this area are obtained from two intensely silicified and cherty 
samples (97R-78 and –80) collected as angular float samples on the shores of two small, east-west trending lakes. 
These samples resembled laminated chert with 10-20% disseminated and veinlet/laminae of pyrite and are interpreted 
to be short distance floats on the basis of their angularity and generally fragile nature.

Northwest of the Little Stull Lake gold deposits along the WBSZ is a zone of multi-element high to moderate contrast 
rock geochemical anomalies centered on a small lake associated with a deflection in the trend of this regional 
deformational zone. This area is interpreted to represent a dilational zone produced during dextral-sense movement 
along the WBSZ. The area is geophysically characterized by a strong, long strike length, northwest trending 
aeromagnetic signature that extends along the WBSZ to the southeast end of Margaret Lake. The strongest portion of 
this aeromagnetic response (2800 nT) occurs at the deflection point. Geochemically the deflection area is marked by 
100th percentile responses for Ni (342 ppm by ICP-AES, 190 ppm by INAA), Cr (1100 ppm), Mg (8.01%), Ba (2600 
ppm), total REE (31.4 ppm) and a modest Ag value of 1.9 ppm. The 99th percentile responses are Mo (7 ppm), Ti 
(1.02% by ICP-AES), P (0.211%), V (361 ppm), Sr (1088 ppm), U (3.4 ppm) and Th (17 ppm) and a 98th percentile 
value for Mo of 11 ppm. A 95th percentile response for Hg (11 ppb) was also obtained. The element assemblages are 
strongly suggestive of a high-Mg source and rock chip samples 97R-23, -24 and –25 were described in the field as 
fine to medium grained, foliated, dark green high-Mg basalt or ultramafic rocks with quartz-carbonate veinlets and 1% 
disseminated pyrite and/or chalcopyrite.

Further to the northwest, the Margaret Lake tonalite intrusion is the site of two distinctive geochemical responses. At 
the west end of Margaret Lake a strong, long strike length, northwest trending airborne EM conductor is coincident 
with a linear aeromagnetic response. The strongest portion of the aeromagnetic response is centered on the north 
shore of a river connecting Margaret Lake and Edmund Lake. At this site, near solid to solid magnetic-rich layers, 
interlayered with basaltic volcanic rocks, are exposed in outcrop chip samples of the magnetite layers and rusty-
weathered interlayered basaltic rock are characterized by 100th percentiles for Fe (26.4%), Mn (19743 ppm), H+ (55.6 
ppb) and specific conductance (154.6 mhos cm-1), and 98th percentiles for Zn (280 ppm by INAA, 294 ppm by ICP-
AES) and Ag (0.9 ppm). A 90th percentile response for Au (27 ppb) was also obtained.

An interesting distribution of geochemical responses is documented from the periphery of the Margaret Lake intrusion, 
particularly at its east and northeast portions. The intrusion contains apparently fracture controlled disseminated pyrite 
and chalcopyrite (sample 97R-27-2) and also has been overprinted by a north-trending laminated pyrite-quartz rich 
mylonite (sample 97R-2). Basaltic volcanic rocks in proximity to the intrusion are marked by 100th percentile responses 
for Mo (41 ppm by INAA, 54 ppm by ICP-AES), Cu (411 ppm), Bi (8 ppm), U (6.9 ppm), Th (22 ppm), V (419 ppm), W 
(900 ppm) and Ca (14.21%). Ninety-ninth percentile responses for Co (82 ppm), Al (10.62%) and Rb (69 ppm) as well 
as a 98th percentile value for Ba (1000 ppm) and Ni (140 ppm) were also observed. There are 90th to 95th percentile 
responses for Au (27-91 ppb) also documented in the rocks peripheral to this intrusion. An aegirine-augite syenite 
intrusion is documented from the are of the north shore of Margaret Lake.

Three geochemically anomalous zones are documented from the Edmund Lake area in association with the WBSZ on 
the east shore, where a sheared and rusty weathered felsic (albitite?) dyke with boudinaged blue, non-mineralized 
quartz veins is marked by the 100th percentile value for Na (5.29%) and the 98th percentile value for K (2.26%). Base 
and precious metal contents were low (97R-57). On an island in central Edmund Lake the 99th percentile response for 
Ni (170 ppm), 98th percentile for Zn (280 ppm) and 95th percentile for Mo (8 ppm by INAA; only 1 ppm by ICP-AES) are 
documented. The ninety-eight and 95th percentiles for Au (91 and 150 ppb, respectively) occur on the east shore of 
Edmund Lake.

	Sharpe Lake Belt

Multi-element, high contrast rock geochemical responses are present along the east-west trending Sharpe Lake belt 
and can be attributed to known gold deposits and anomalous geophysical features documented by Hosain (1997). The 
area between the northwest shore of Monument Bay west to the southern part of Twin Lakes is characterized by 
significant geochemical response from both the Twin Lakes and Seeber River gold deposits as well as the altered host 
rocks which include iron formation. The Monument Bay area is marked by 100th percentile responses for Ba (930 
ppm), Sr (847 ppm) and Al (10.16%), a 560 ppm As analyses (99th percentile) and 98th percentiles for Hg (31 ppb), Bi 
(5 ppm), Th (17 ppm), REE (402.8 ppm), K (3.98%), P. (0.165%), Na (4.07%) and specific conductance 35.5 mhos 
cm-1. Pb (33 ppm), Sb (7.4 ppm) and U (4.3 ppm) 95th percentile responses were also documented.

Further west in the Twin Lakes area multiple geochemical responses are obtained. Co (85 ppm), Th (26 ppm), REE 
(529.6 ppm), W (730 ppm), Hf (12 ppm), P (0.193%) and a low contrast Ta value of 2.3 ppm represent 100th percentile 
responses in this area. The 99th percentiles of As (890 ppm), Rb (160 ppm), Pb (58 ppm) and Al (9.84%), the 98th 
percentiles of U (5.4 ppm) and K (3.9%) as well as the 2.6 ppm Sb (90th percentile) response are all indicative of 
mineralized and altered stratigraphy in the Twin Lakes area.

In the area south of Twin Lakes, near the southern margin of the belt significant base and precious metal responses 
are observed. The 100th percentile responses for Cs (22 ppm) and Mn (3476 ppm) occur in association with 99th 
percentile values for Cu (199 ppm) and Ni (192 ppm), 98th percentiles for As (820 ppm), Ti (1.12%) and specific 
conductance (35.5 mhos cm-1). A 27 ppb Au response (95th percentile) also occurs in this area. Notably, there are 
anomalous geophysical responses in the area of these geochemical anomalies, specifically east-west trending 
medium strength airborne EM conductors that are transected by a northwest-southeast trending fault (Hosain, 1997; 
cf. map OF97-4-21). The geochemical signatures observed in this area are likely related to these conductors and/or 
the fault. Alternatively, the signatures are developed in response to mineralized faults or shear zones that occur at or 
near the southern margin of the belt where significant rheologic differences exist between primarily mafic to 
intermediate volcanic rocks of the Sharpe Lake belt and the granitic intrusive terrane to the south.

Further west along the southern margin of the belt is a zone devoid of geophysical conductors or anomalous magnetic 
response but characterized by multiple high contrast geochemical anomalies. The area is south of Makataysip Lake 
and has what may be described as the most significant responses identified in the 1997 rock geochemical survey. The 
Au (40 ppb), As (2000 ppm), Zn (276 ppm by INAA and 146 ppm by ICP-AES), U (6.7 ppm), Ni (360 ppm), Cr (1200 
ppm), K (4.97%), Br (19 ppm) and specific conductance (44.8 mhos cm-1) responses are 100th percentiles. 
Additionally, a 99th percentile Th (22 ppm) response and 98th percentiles for Sb (10 ppm), Co (66 ppm), Cs (6 ppm), Ba 
(800 ppm) and W (690 ppm) and a 95th percentile Rb (110 ppm) response were obtained. West of Makataysip Lake 
also along the southern margin of the belt, 100th percentile responses for Ni (386 ppm), Mg (9.28%), Bi (8 ppm) and a 
strong REE (98th percentile, 402.8 ppm) response identifies another altered and mineralized site where high-Mg 
basalts or ultramafic rocks are associated with sulphide mineralized and otherwise altered rocks. The zone south of 
Makataysip Lake is a precious metal target with similarities in terms of indicator elements to the Twin Lakes and 
Monument Bay areas. Two rock chip samples were collected at site 199 and comprise a rusty weathered rhyolite 
“dyke”(?) without visible sulphide minerals and a grey, silicified basalt erratic with 25% pyrite. Both samples were 
collected at the edge of a shallow, linear lake and are interpreted as short transport erratics. Significant precious metal 
responses are attributed to blue, fine-grained quartz veins with pyrite laminae and blue, boudinaged quartz veins with 
disseminated blocky arsenopyrite at the vein-wallrock contact.

The west shore of Makataysip is marked by a 6700 nT circular aeromagnetic anomaly that is transected at its 
northeast side by a northwest-southeast trending fault. There are no EM conductors associated with this magnetic 
anomaly (Hosain, 1997; cf., Map OF97-4-20). Moderate geochemical responses were obtained from the area of this 
anomaly. The 100th percentile responses for Fe (13.1%), Ti (1.34%), V (527 ppm) and Sc (49 ppm), 99th percentile 
responses for Zn (230 ppm by INAA, 121 ppm by ICP-AES) and Y (46 ppm) and a 95th percentile response for Co.

The central portion and the east end of Sharpe Lake are characterized by long strike length medium to strong airborne 
EM conductors. These conductors define a fold nose at their eastern extremity and at this location are coincident with 
a folded, linear aeromagnetic anomaly that trends northwest from Sharpe Lake and passes to the east of Barclay Lake 
(Hosain, 1997; cf., Map OF97-4-19). Hosain (1997) reports no diamond drill testing of these electromagnetic and 
aeromagnetic anomalies. The central and east Sharpe Lake area contains good base and precious metal geochemical 
responses characterized by 100th percentiles for Cu (231 ppm) and Pb (64 ppm), a 99th percentile for Mn (2929 ppm) 
and 98th percentiles for Au (31 ppb), Co (66 ppm), Cr (370 ppm), Zn (230 ppm), W (690 ppm), Sc (41 ppm) and Hf (7 
ppm). Significant 95th percentile responses include As (520 ppm), Sb (7.4 ppm), Ni (188 ppm), Mg (5.62%) and Br (8.9 
ppm).

The north shore of the west end of Sharpe Lake is characterized by long and short airborne EM conductors coincident 
with a linear east-west trending aeromagnetic anomaly. Diamond drill testing of the EM conductors on the west end of 
these features intersected altered ultramafic rocks with magnetite (Hosain, 1997). Approximately 2-3 km north of these 
geophysical conductors are a second set of long strike length airborne EM conductors that extend to the west of the 
south end of Webber Lake. In this area the airborne EM conductors appear as moderate to short strike length 
conductors confirmed by subsequent ground EM follow-up. Diamond drill testing of these shorter strike length 
conductors intersected rhyolite, andesite and argillite with graphitic or “earthy” pyrite. A 0.6 m intersection assayed 
0.29% Cu and 0.4% Zn (Hosain, 1997; of map OF97-4-19).

The conductive and magnetically anomalous zones are marked by 100th percentile responses for Hg (83 ppb; 99th 
percentile =54 ppb), Ca (16.55%), Rb (170 ppb), Ag (1 ppm) and the highest Sb analysis (63 ppm) in the 1997 rock 
geochemical survey. The area also contain a 99th percentile value for U (5.6 ppm) and 98th percentiles for Pb (41 
ppm), V (298 ppm), Mg 5.62%), Sc (41 ppm) and Br (12 ppm).

The relatively high (99th percentile) U response in the western Sharpe Lake area is related to samples collected from 
sites 249 and 266. At these stations bleached, yellow stained (uranium oxide?) and fractured granites with 
approximately 20% disseminated and veinlet pyrite were observed. The 63 ppm Sb analysis also came from site 249.

A small area of greenstone belt is present north of western Sharpe Lake at Barclay Lake. The west shore of this lake 
is characterized by a small, circular aeromagnetic feature and moderate to strong airborne EM conductors on the north 
end of the lake. One of these conductors is coincident with the northwest arm of a linear aeromagnetic anomaly that is 
also present on the north-central shore of Sharpe Lake.

A single outcrop chip sample collected from outcrop at the edge of the western shoreline is marked by a 99th percentile 
response for Ca (14%) and 98th percentiles for Mn (2789 ppm) and Ag (0.7 ppm). The field description for the hand 
sample collected at this site identifies a strongly foliated diorite that is locally rusty weathered with epidote and 
carbonate alteration and 1% pyrite.

Conclusions and Recommendations

The following conclusions are evident from a preliminary assessment of 1997 rock geochemical data:

1.	The host rocks to the Little Stull Lake gold deposit in the Edmund Lake belt, and the Twin Lakes and Seeber River 
gold deposits in the Sharpe Lake belt are characterized by a diverse suite of “ore-related” elements. These 
elements (Au, As and Sb) are related to dispersion about the mineralized zones, whereas elements such as K and 
Al reflect styles of alteration of the host rocks. The association of indicator elements, such as the REE, with the 
gold zones provides a possible discriminator between “barren” and Au-mineralized alteration zones.

2.	Unique geophysical and coincident geochemical anomalies have delineated prospective areas along the WBSZ in 
the Edmund Lake belt. At the “deflection” point along the WBSZ geochemical anomalies are coincident with 
significant airborne geophysical responses.

3.	Unique lithologies such as high-Mg basalts or perhaps ultramafic rocks, in association with the WBSZ or along the 
southern margin of the Sharpe Lake belt have been identified (Mg, Ni, Cr, Co, Fe), some of which are associated 
with 100th percentile “ore-elements”.

4.	The potential for the Margaret Lake intrusion to be a heat or metal source for mineralizing fluids can be assessed 
on the basis of the distribution of Cu and Mo in the intrusion and in basaltic volcanic rocks at the periphery of the 
intrusion. The altered quartz-feldspar porphyry intrusion on the northwest end of Little Stull may be interpreted as 
a metal source for the Little Stull Lake gold deposits (or other mineralized zones) given its proximity to the gold 
mineralized zones as well as its anomalous geochemical signatures.

5.	The central to west portions of Sharpe Lake are marked by very high Sb and Hg contents. That are coincident with 
anomalous geophysical conductors. These responses should be carefully assessed.

6.	The southern area of the Sharpe Lake greenstone belt is marked by significant rock geochemical responses. The 
area south and west of Makataysip Lake should be carefully explored for structurally controlled gold 
mineralization. It is likely that the south contact between volcanic rocks and granitic intrusive rocks to the south is 
faulted.

7.	The circular aeromagnetic response on the west shore of Makataysip Lake should be reconnoitered to determine 
the nature of the rocks in this area and their metallogenetic potential.

8.	The geochemical responses on the east and west shores of Edmund Lake as well as islands in the central portion 
of the lake, coupled with deformation related to the WBSZ and the association of ultramafic rocks requires detailed 
assessment.

9.	The contact between the Oxford Lake Group sedimentary and volcanic subgroups and the Hayes River basalts is 
an important metallogenetic feature in the Sharpe Lake belt. This contact localizes the Twin Lakes and Seeber 
River gold deposits and numerous base-and precious metal geochemical anomalies. It should be considered as 
highly prospective.

TILL GEOCHEMICAL SURVEY
Introduction

Till samples were collected for geochemical and kimberlite indicator mineral analyses at 152 of the 287 field stops 
made in the Edmund Lake and Sharpe Lake greenstone belts. Observations on the ice-flow history, indicated by the 
orientation of glacial striations and drumlins, as well as observations on the Quaternary geology and sediment 
provenance relevant to the interpretation of the till geochemistry and kimberlite indicator mineral distribution were an 
integral component of the field work. As in previous years, particular attention and effort was made to collect only 
those sediment samples that met the most rigorous criteria of what might be classified as till.

Methods
	Field Methods

All till samples were collected from hand-dug pits. The pits were dug to bedrock, to a maximum depth of about one 
metre or until the first unoxidized gray to buff, silty C-horizon till was intersected.  Of the 152 till samples collected, 121 
were obtained from under a relatively impervious layer of fine textured glaciolacustrine clay or silty clay. For this 
reason these samples are considered to be relatively unweathered C-horizon tills.  Of the remaining 31 samples only 
11 (6, 23, 28, 62, 79, 95, 109, 189, 196, 199 and 256) showed visible signs of oxidation. A half kilogram of till was 
collected for geochemical analyses and an 11 litre pail of till was collected for diamond indicator mineral processing 
from each site.

	Laboratory Methods

Two size fractions, a <2µm (clay-sized) fraction and a <63µm (silt and clay) sized fraction, were prepared in the 
Manitoba Energy and Mines rock laboratory. The <2µm fraction was prepared following standard procedures of 
centrifuging and decanting. The <63µm fraction was prepared by dry sieving on a 63µm stainless steel sieve. The 
<2µm fraction was analyzed by ICP-AES (34 element suite). In addition arsenic was analyzed by hydride generation 
and mercury was analyzed by cold vapour. The <63µm fraction was analyzed by INAA (Au +34 element suite).

Results
	<2µm Fraction

The results of the analyses on the <2µm size fraction are listed in Appendix 1. The data was divided into an Edmund 
Lake and a Sharpe Lake data set because of anticipated differences in the regional  background. The two data sets 
have been plotted on the same map. Only those elements with a ‘sufficient’ number of determinations above the 
detection limits to make a map are shown in the accompanying bubble plots. In all instances, values at or below the 
detection limits were taken to be .50 times that value. Percentile bubble plots for the analytical data contained in 
Appendix 1 are presented in Appendix 2.

	Edmund Lake area

The highest copper value, at 143 ppm, though only marginally anomalous, is found over the Hayes River basalts at the 
southeastern end of the belt associated with several other marginally anomalous samples. The highest lead value (26 
ppm) occurs in the area south of the eastern tip of Margaret Lake in sample 15, which was collected over granite 
bedrock. Zinc concentrations are highest at site 7, situated near the southern margin of the belt, and a single sample 
(site 52) over the Wolf Bay Shear Zone is also considered marginally anomalous. The only significant nickel value at 
60 ppm, occurs at site 92 coincident with the previously mentioned copper anomaly. Cobalt is also slightly elevated at 
site 92 but the highest value is found over the shear zone south of Margaret Lake coincident with elevated iron values. 
Manganese is high at site 15 coincident with elevated lead values. Anomalous manganese values also occur at site 78 
near the eastern end of the belt. Barium is highest at site 6 south of Little Stull Lake and several marginally anomalous 
samples are found associated with the Wolf Bay Shear Zone between little Stull Lake and Margaret Lake. Sites 6 and 
85, near the east end of the belt, and site 28 south of Margaret Lake are anomalous in chromium, coincident with 
elevated nickel values. Sites 6 and 28 also have elevated vanadium levels. The highest mercury value, though only 
marginally anomalous, occurs at site 15 coincident with elevated lead and manganese values.

Other notable anomalous values include aluminum, sodium, lithium and scandium at site 28 and  aluminum, lithium 
and scandium at site 6. Magnesium is elevated in several samples collected over the Hayes River basalt and down ice 
from the Wolf Bay Shear Zone at the east end of the belt. Sample 15 is anomalous in sodium and yttrium in addition to 
the elements mentioned previously. The highest arsenic levels (60.9 ppm) occurs at site 90 collected over the shear 
zone southeast of Little Stull Lake. Other sites with anomalous arsenic occur down ice from this same area.

	Sharpe Lake area

A single sample copper anomaly is found at site 200 located southwest of Makataysip Lake. A multi-sample copper 
anomaly occurs north of Monument Bay that appears to be a continuation of the prominent anomaly described 
previously at the southeast end of the Edmund Lake belt. Lead and zinc values are high (up to 17 ppm and 99 ppm 
respectively) in several samples overlying the Oxford Lake sedimentary rocks east and southeast of Makataysip Lake. 
The highest zinc value is a single sample anomaly collected near the east end of Sharpe Lake. The highest nickel 
value (122 ppm) is from site 200 coincident with elevated copper. Several samples south of Makataysip Lake to the 
east of sample 200 and also underlain by Hayes River basalts have elevated nickel, cobalt, iron, barium, chromium, 
vanadium, aluminum, lithium, and scandium values. 

Sample 217 located near the east end of Sharpe Lake is anomalous in zinc, barium, chromium, lanthanum, potassium, 
strontium, as well as, yttrium, lithium, niobium, and scandium. Sample 223 is anomalous in mercury and sodium.

	<63 µm Fraction

Analytical results (INAA) for the <63 micron fraction are listed in Appendix 3. Percentile bubble plots based on these 
data are reproduced in Appendix 4.

	Edmund Lake area

The highest concentration of  gold (54 ppb) occurs at site 90, located on the Wolf Bay Shear Zone, near the east end 
of  Little Stull Lake. Other anomalous concentrations of gold are found down ice from site 90 and along the shear zone 
towards Margaret Lake. Elevated gold values south of Little Stull Lake are coincident with high arsenic values in the 
same area, although the highest concentrations occur, not in association with known mineralization at sites 1 and 71, 
but farther east at site 90. Elevated concentrations of arsenic across the Hayes River basalt, south of Little Stull Lake 
may be related to glacial dispersion from the Wolf Bay Shear Zone or to unknown mineralization in the area.

Barium, cobalt, chromium, cesium, iron, molybdenum, rubidium, scandium, thorium, uranium and the rare earth 
elements are highly anomalous at site 6, south of Little Stull Lake. Cobalt, chromium, iron, hafnium, sodium, scandium, 
tantalum, thorium, uranium and the rare earth elements are anomalous in several samples south of the eastern end of 
Margaret Lake, notably at site 28. Molybdenum concentrations up to 9 ppm occur in several samples over the Hayes 
River basalt, south of Little Stull Lake and may be related to glacial dispersion or local variation in the bedrock. Zinc 
and antimony attain their highest values (408 ppm and .6 ppm) at site 1, adjacent to known gold mineralization along 
the south shore of Little Stull Lake. Sample 2, collected to the north of the Wolf Bay Shear Zone, is also anomalous in 
zinc.

	Sharpe Lake area

The highest concentration of gold (60 ppb) in the till was not found in the area of known gold occurrences at 
Monument Bay, but over the granite in the area south of Barclay Lake. Arsenic and antimony values are also 
anomalous in several samples around Barclay Lake. The highest arsenic values are associated with a multi-sample 
multi-element anomaly south of Makataysip Lake. Other anomalous elements in this area include barium, bromine, 
cobalt, chromium, cesium, iron, hafnium, sodium, rubidium, scandium, thorium, uranium and the rare earth elements. 
Other notable anomalies include a multi-element anomaly of barium, cobalt, chromium, cesium, iron, molybdenum, 
sodium, rubidium, scandium, tantalum, thorium and rare earth elements at site 217 near the east end of Sharpe Lake. 
Samples  254, 262 and 264, south of Webber Lake are noteworthy for their high concentrations of molybdenum.

Calcium, with concentrations between 1 and 20 percent, is derived almost exclusively from Paleozoic carbonate rocks 
in the Hudson Bay Lowland and is an indicator of long distance glacial transport. The well developed drumlins in the 
Monument Bay area have slightly elevated calcium levels suggesting they may have a higher allochthonous 
component than the non drumlinized till. This conclusion is not supported by the carbonate content of the drumlins in 
the Barclay Lake area.

Synthesis
	Edmund Lake Area

A prominent multi-element and multi-sample anomaly comprising Cu, Pb, Zn, Ni, Co, Fe, Mn, Ba, Cr, Hg, Mo, Mg and  
As is found over the Hayes River basalt south of Little Stull Lake. A similar multi-sample anomaly of  Pb, Ni, Co, Fe, 
Mn, Cr, V and Hg is situated over the Hayes River basalt south of the east end of Margaret Lake. Approximately 
halfway between Margaret and Little Stull Lakes, over the Hayes River basalt, is a minor multi-sample anomaly of Ba, 
Br, Co, Mo, Ta, Th, U, Zn, K and Ti. The Wolf Bay Shear Zone is characterized by anomalous levels of Au, As and Sb.

	Sharpe Lake Area

Au is anomalous south of Barclay Lake in an area of no known supracrustal rocks. The till occurs in drumlins and the 
anomaly may be the result of long distance glacial transport from some unknown source, possibly the Edmund-
Margaret Lake area or farther north. A prominent multi-element multi-sample anomaly comprising Cu, Ni, V, As, Ba, 
Br, Co, Cr, Fe, Cs, Rb, Sc, Th, Al, Li and U occurs over the Hayes River basalt south of Makataysip Lake. In the same 
area over the Oxford Lake sedimentary rocks anomalous levels of Pb, Zn, and Y occur. 

The drumlinized till in the Monument Bay area is anomalous only in copper. Copper distribution in this area may be 
part of a southerly trending glacial dispersion train emanating from the Hayes River basalts south of Little Stull Lake. 
Although, the generally low concentrations of other elements in the Monument Bay area suggests that the drumlinized 
till in this area has a larger allochthonous component than other areas and does not reflect the composition of the 
underlying bedrock to the same degree as the nondrumlinized till; a conclusion borne out in part by elevated levels of 
calcium in this area compared to other areas such as south of  Little Stull Lake. However, the low calcium levels of the 
drumlinized till in the Barclay Lake area does not support this conclusion.


B-HORIZON SOIL GEOCHEMICAL SURVEY
Introduction

B-horizon soil samples have been used extensively during geochemical exploration programs for base and precious 
metals as well as other commodity types. Routinely, these samples were sieved to -80 mesh and analysed for 
numerous elements by AAS or ICP-AES, subsequent to an aqua regia digest. Other dissolutions were also utilized 
including a number of phase specific and sequential digestions.

The b-horizon geochemical database created for Operation Superior samples collected in 1997 is based upon the 
enzyme leach process. This analysis is a phase specific approach to the delineation of metal-enriched zones within b-
horizon samples. The enzyme leach data, like data generated from all other analytical approaches in the dataset, are 
interpreted from each of two sub-areas within the 1997 survey area.

	Enzyme Leach

This process is a phase-specific leach that preferentially attacks amorphous manganese oxide coatings on mineral 
grains thereby liberating trace metals that are trapped in this material. Amorphous manganese oxide represents an 
efficient chemical sieve or trap for cations, anions and polar molecules because of its large surface area and the 
random distribution of charges on this surface. The trace elements that are trapped or complexed on the amorphous 
manganese oxides are interpreted to represent the chemical signatures of buried, oxidizing mineralization at depth, 
rather than signatures originating from a transported overburden source, such as till. It should be noted, however, that 
the geochemical signature within the b-horizon may be strongly affected by the weathering of till and the subsequent 
downward movement of metals as a result. This could produce a “transported” till geochemical signature in 
combination with site specific mineralization-related geochemical signatures and a composite signature overall. The 
possible contribution of parent material composition to the overall enzyme leach signature is not well understood.

Most of the amorphous manganese oxide is developed in the b-horizon, where studies in both arid and humid 
geological and climatic environments have established that mineral particles within this soil horizon are coated with this 
authigenic material. The a-soil horizon may not reflect geochemical anomalies identified in the b-horizon since a-
horizon is fairly rapidly leached of its metallic components which are carried downwards, perhaps as humic- or fulvic-
acid compounds (humates/fulvates?), and trapped or sieved as they encounter the amorphous Mn-oxide coatings on 
mineral grains in the b-horizon. The chemical composition of the a-horizon is significantly impacted by the metal 
contents of vegetation contributing litter to the forest floor. This litter will reflect metals obtained by vegetation during 
nutrient acquisition from soil horizons tapped by root systems. Accordingly, the a-horizon geochemical signature will 
reflect the ability of various species to acquire and store metals until such time as they are dropped to the forest floor, 
decompose and move downward in the soil profile. This source of metal may, therefore, reflect a transported metal 
signature representing a clastic component within an exotic till or lacustrine clay rather than a buried mineralization 
signature.

The diffusion of relatively volatile metal phases or metals transported by gases consisting of Hg-vapour, Co2, Rn, He, 
N, 02, C04, Ar and S-compounds, away from an oxidizing zone of mineralization, undoubtedly proceeds as a result of a 
number of processes. Metal transport may be effected by the influence of an electrochemical or self-potential cell, or 
as components in soil gases derived from mantle de-gassing (cf. Gold and Soter, 1980; “geogas”, Malmquist and 
Kristiansson, 1984; “earth-gas”, Wang et al., 1997). The role of shallow groundwater as the transport medium for 
metals from source to surface is also being investigated (Stewart Hamilton, pers. comm.). Metals carried by one or 
more of these mechanisms will be adsorbed by the amorphous Mn-oxide, enriching this portion of the b-horizon in 
metals. Native gold and mercury in the soil profile will not be digested using the enzyme leach.

The leachate from the b-horizon soil is analyzed by ICP-MS for 59 elements at detection limits in the parts per billion 
range. Clark (1992, 1993) provides theory and application of the enzyme leach method.

Sample Collection

B-horizon soil geochemical samples were collected from the same pit dug for the till samples. The b-horizon was 
isolated on a clean face of one or more walls of the pit and then scooped into a labelled, medium-sized, ZIPLOC 
sample bag that was filled. Care was taken not to include any organic material either from the overlying humus or from 
forest litter when collecting this inorganic sample. This precaution was considered particularly important for enzyme 
leach analyses where considerable variance can be added to the data by mixing organic and inorganic material. The 
b-horizon in the survey areas ranged in colour from orange to chocolate brown with less intense variants of these 
colours.

At some sampling sites there was a 3-5 cm zone of mixing between organic and inorganic soil layers. In these 
instances the b-horizon sample was collected from below the zone of mixing. Another variant in b-horizon sampling is 
the slumped, contorted and mixed nature of the most decomposed portions of the b-horizon with less oxidized, usually 
lower b-horizon material. This was attributed to either frost-jacking or to a variation of soft sediment deformation. In 
these instances the b-horizon sample comprises the most strongly oxidized b-horizon material that was inevitably 
mixed with less oxidized material.

Duplicate samples were collected every tenth site.


Sample Preparation and Analysis

At the end of the day, samples were returned to camp and stored in a shaded low lying area out of the direct rays of 
the sun, where temperatures did not exceed 40oC. This temperature is considered to represent the upper limit for 
samples to be analysed by the enzyme leach method. Temperatures exceeding 40oC will result in volatilizing metal-
bearing compounds from the sample (Bob Clarke, Activation Laboratories Ltd., pers. comm.).

B-horizon soil samples were shipped to the Manitoba Geological Services Branch laboratories by refrigerated 
transport, where they were air dried at less than 40oC and sieved to obtain the -60 mesh size fraction. The -60 mesh 
portion was forwarded to Activation Laboratories Ltd. for enzyme leach-ICP-MS analysis. A separate -80 mesh aliquot 
was submitted to the Manitoba Geological Services Branch laboratory for the measurement of pH and conductivity. 
The pH and conductivity measurements were corrected and converted to H+ and specific conductance using the 
formula of Govett (1976) and reproduced with examples in Govett et al., (1984).

Geochemical data is listed in Appendix 1 and analyses for field duplicate samples are listed in Appendix 2. Percentile 
bubble plots appear in Appendix 3. With the exception of the hydrogen ion (H+) and specific conductance (K) no other 
analyses were performed on the b-horizon soils.

Results
	Edmund Lake Belt

The enzyme leach analysis of b-horizon soil samples in the Edmund Lake belt has identified multiple sites of high 
percentile responses that correspond to the locations of known mineralization at Little Stull Lake and sites identified as 
geochemically anomalous in the rock geochemical survey.

The Little Stull Lake gold deposits are marked by high percentile responses for numerous “commodity” elements and 
other elements indicative of associated alteration and structural overprinting (WBSZ) of the mineralized host rocks. 
Commodity and “ore-related” element responses include 100th percentile values for As (137 ppb), Mo (94 ppb), Pb (33 
ppb), Ga (23 ppb), Ni (79 ppb), a 99th percentile for Sb (3 ppb) and a 98th percentile of 29 ppb for Co. Additional 
responses include the 100th percentile for V (349 ppb, 99th percentile of 262 ppb, also) and Nb (12 ppb), 99th 
percentiles for Ba (932 ppb) and Cs (6 ppb) and a 98th percentile of 76 ppb for Li. Interestingly, the area of the Little 
Stull Lake gold deposits would have been deemed “anomalous” solely on the basis of a 100th percentile response for 
specific conductance (30.75 mhos cm-1).

Due west of the Little Stull Lake area, 100th percentile values for Sr (1206 ppb; 99th percentile of 872 ppb also) and I 
(373 ppb) have been observed. Southwest of Little Stull Lake in the contact area of the greenstone belt and granitic 
intrusive terrane there are multiple 98th (17 ppb) to 95th (12 ppb) percentile responses for Mo.

As identified in the rock geochemical survey, the area south and east of Little Stull Lake to the Manitoba-Ontario 
provincial border is also characterized by an extensive list of elements determined by ICM-MS in b-horizon soils 
subsequent to enzyme leaching. An affiliation to sulphide mineralization is indicated by 100th percentile responses for 
Cu (150 ppb; 99th percentile of 115 ppb as well), Pb (33 ppb), Ni (79 ppb), Mo (94 ppb), Sb (5 ppb; 99th percentile of 3 
ppb) and Ga (23 ppb). Alteration-, structural-, or lithology- related responses include 100th percentile values for Li (134 
ppb), Ti (4394 ppb), V (349 ppb), Sr (1206 ppb), Y (104 ppb), Nb (12 ppb) and the REE (1070 ppb). Other significant 
responses include 99th percentiles for Rb (151 ppb), Cs (6 ppb) and Mn (2711 ppb); a 98th percentile for As (39 ppb) 
and both 99th and 98th percentile responses for specific conductance (30.37 and 29 mhos cm-1, respectively). 
Southwest of Little Stull Lake at or near the margin of the greenstone belt, a 100th percentile response for Sc (10539 
ppb) is documented. High Sc contents have been previously been observed in association with faults and shear zones 
and is suggestive that the nature of the greenstone belt/granitic intrusive contact is faulted.

The area of the deflection of the WBSZ is marked by only two commodity element responses and both of these are 
interpreted to be low contrast signatures. These are Cd (100th and 98th percentiles of 3 and 1.8 ppb, respectively) and 
the 98th percentile for Ga (11 ppb). Other significant responses include 98th percentiles for Ba (845 ppb) and Ti (1536 
ppb); three 95th percentile (6 ppb) Nb responses and a 100th percentile Br response of 1161 ppb that occurs west of 
the WBSZ deflection. Anomalous rock geochemical response in the general area of the Margaret Lake tonalite 
intrusion was postulated as representative of mineralization and alteration that accompanied the emplacement of this 
granite. Some of the observed geochemical variance in the dataset, however, was attributed to samples collected from 
outcropping magnetite-rich iron formation at the west end of Margaret Lake. Enzyme leach responses in the vicinity of 
this iron formation include 100th percentiles for Co (43 ppb), U (7 ppb), Rb (177 ppb), Hf (11 ppb) and H+ (8.9 ppb). 
The area peripheral to the Margaret Lake intrusion is marked by the 100th and 99th percentile values for Cl (46463 ppb) 
and 10340 ppb, respectively), the 100th percentile for Co (43 ppb), Zn (214 ppb) and Cu (150 ppb). Additional 
significant “peripheral” response include 99th percentiles for Mo (18 ppb), Li (79 ppb), Sc (3883 ppb), Ti (1558 ppb) and 
H+ (4.47 ppb). A 98th percentile for Zr (93 ppb) and Pb (21 ppb) were also documented. Southeast of the Margeret 
Lake intrusion near the WBSZ, a 100th percentile response (3726 ppb) was obtained.

The east and west shores of Edmund Lake and to a lesser extent islands in the central portion of the Lake are marked 
by geochemical signatures for elements generally interpreted to be associated with faults and shear zones. This is not 
unreasonable since the WBSZ transects the lake in a northwest to southeast altitude. These structurally-related 
elements include 100th percentile values for Sc (10539 ppb), Zr (291 ppb), Rb (177 ppb), Li (134 ppb), Hf (11 ppb; 99th 
percentile = 6 ppb), REE (1070 ppb) and the 99th percentile for Nb (10 ppb). Commodity related responses include the 
100th percentile for Zn (214 ppb), Th (79 ppb – west and central Edmund Lake), U (7 ppb) and Ag (1.1 ppb) albeit the 
Ag response is very low. The 99th percentile values for Pb (24 ppb), Ga (15 ppb) and Cs (6 ppb) and specific 
conductance (30.4 mhos cm-1) and the 98th percentile for Ba (845 ppb) also characterize the Edmund Lake area. A 
4394 ppb Ti (100th percentile) response from the west shore of the lake in interpreted to indicate the presence of high-
Mg basalts or ultramafic intrusions that are documented from islands in the central portion of the lake.

Other areas of interest in the Edmund Lake belt include 100th percentile values for Cl (46463 ppb), Mn (3726 ppb), Br 
(1161 ppb), Ba (1130 ppb) and Cd (3 ppb) in the Kistigan Lake area. A 100th percentile response for Ba also occurs 
west of Kistigan approximately one-half way to Margaret Lake. A 99th percentile for H+ (4.47 ppb) was also 
documented from the Kistigan Lake area. A 98th REE (569 ppb) percentile was obtained west of Kistigan Lake in 
granitic intrusive terrane.

A 100th percentile for I (373 ppb) occurs southwest of Rorke Lake and a 99th percentile (156 ppb) is documented on 
the east-west division between Rorke Lake and Kistigan Lake.

	Sharpe Lake Belt

The Sharpe Lake belt is marked by excellent correspondence between enzyme leach geochemical signatures and 
bedrock anomalies identified in the rock geochemical survey. In this regard it is similar to the results for the Edmund 
Lake greenstone belt.

The Monument Bay area represents the probable eastern extension of a stratigraphic and structural rock “package” 
that hosts the Twin Lakes and Seeber River gold deposits. Mineralization occurs at or close to the contact between 
rocks of the volcanic and sedimentary subgroups, Oxford Lake Group. This contact area is the site of numerous 
geochemical anomalies as defined by the enzyme leach process, some of which are suggestive of a fault related 
control to the mineralization.

The contact area is marked by 100th percentile responses for Sc (7841 ppb), Ti (2922 ppb), Ga (19 ppb) and Mo (70 
ppb – 2 responses). Other significant responses include a 99th percentile for Hf (4 ppb) and 3 – 98th percentile Zr 
responses (93 ppb). In the area north of Monument Bay, west towards southern Twin Lakes, a string of 100th (4884 
ppb) and 98th (1555 ppb) percentile responses are documented for Mn. A similar pattern is observed for Sr with 95th to 
98th percentile responses (709 to 911 ppb) and V (98th percentiles, 270 ppb) occurring in this area. Additional “point 
source” responses occur in the northern area of Monument Bay and these include Zn (100th percentile, 73 ppb), 99th 
percentiles for U (4 ppb) and Rb (131 ppb) and 98th percentiles for Pb (19 ppb), Nb (10 ppb) and Li (72 ppb). The 
southern portion of the Monument Bay area is marked by a 100th and 99th percentile response for Cl (14569 and 6657 
ppb, respectively) and a 98th percentile for As (365 ppb). Further south of Monument Bay, near the southern margin of 
the Sharpe Lake belt, there are two 100th percentile Cu responses (215 ppb) and a single 100th As percentile (114 
ppb). As in many of the other areas in the Edmund Lake belt a signficant (98th percentile) specific conductance 
response is obtained (25.7 mhos) near the northwest corner of Monument Bay.

The Twin Lakes and Seeber Ricer gold deposits occur near the southern end of the Twin Lakes, which is 
characterized by multiple commodity and structurally related enzyme leach element responses. Commodity element 
responses include 100th percentiles for Pb (21 ppb) and Th (32 ppb), 99th percentiles for Zn (61 ppb), Ga (16 ppb) and 
U (4 ppb) and 98th percentiles for Co (27 ppb) and Mo (28 ppb). The Mo signature forms an eastward trend towards 
Monument Bay at or near the Oxford Lake volcanic-sedimentary rock contact along which multiple 98th and 95th 
percentile (13 ppb) are present. Structurally-related elements in the Twin Lakes area include a 100th percentile 
response for Nb (11 ppb), 99th percentiles for Sc (7180 ppb) and Ti (2436 ppb) and 98th percentiles for Rb (104 ppb) 
and Y (67 ppb).

South of the immediate Twin Lakes area, multiple moderate to high contrast geochemical responses are documented. 
These signatures include 100th percentiles for As (114 ppb), Ag (1.8 ppb), Cs (11 ppb), Y (77 ppb) and REE (670 ppb), 
99th percentiles for Sr (974 ppb), I (200 ppb), Cu (99 ppb) and specific conductance (25.7 mhos cm-1, also a 98th 
percentile of 26.1 mhos cm-1) and 98th percentiles for Ga (15 ppb), Nb (10 ppb), Pb (19 ppb –2 responses), Th (23 
ppb), Br (365 ppb) and H+ (4.7 ppb).

The area of the greenstone belt contact with the granitic intrusions to the south is marked by 100th percentiles for Ni 
(83 ppb), Co (37 ppb, 99th percentile of 34 ppb) and V (376 ppb). Approximately 5-6 km east of this V response is a 
second 100th percentile signature. The 99th percentile response for Li (88 ppb) and the 98th percentiles for Sc (5601 
ppb) and Ti (2434 ppb) are suggestive of a high-Mg source rock possibly occurring at the faulted belt contact.

The west shore of Makataysip Lake is marked by a circular 6700 nT aeromagnetic anomaly and multiple anomalous 
rock geochemical signatures. Relatively few elements respond in enzyme leach b-horizon geochemical data. The 100th 
percentile response for Co (37 ppb), relatively low contrast 99th percentile for H+ (5 ppb) and 98th percentile responses 
for Cl (6406 ppb), Ba (841 ppb) and Rb (104 ppb) are the only significant responses. A low 1.8 ppb Ag response (100th 
percentile) is also observed.

This paucity of anomalous responses on the west shore is reversed, however, in the area south of Makataysip Lake at 
or near the southern margin of the belt. This site was also marked by multi-sample, multi-element rock geochemical 
anomalies. In the b-horizon enzyme leach data 100th percentile values are observed for Zr (148 ppb), Y (77 ppb), Rb 
(159 ppb), Ba (1240 ppb); H+ ( 7ppb) and a very low and probably insignificant Ag response of 0.8 ppb. These 
elements are dominantly those associated with faults and suggest the nature of the southern margin of the belt in this 
area is in fault contact with granitic intrusions to the south. The 99th percentile REE response of 531 ppb and the 98th 
percentile for Nb (10 ppb) are further evidence to support the structural nature of the contact. Commodity element 
responses include 99th percentiles for Ni (56 ppb), Ga (16 ppb) and a low 1.3 ppb for Cd. Pb (19 ppb), Th (23 ppb), Ti 
(2434 ppb) and U (3 ppb) represent 98th percentile responses in this area. The 100th percentile for Cl (14569 ppb) 
occurs in this area as well and is at or near the southern contact of Oxford Group sedimentary and volcanic rocks. 
West of Makataysip Lake at the southern belt margin, 99th percentile As (63 ppb), and 98 percentile Ti (2434 ppb) and 
Ga (15 ppb) are documented.

Moderate to low contrast base and precious metal signatures occur in the area of the east end of Sharpe Lake. The 
100th percentile values for Ni (83 ppb), Sb (28 ppb), Sr (1803 ppb), I (226 ppb), Ba (1240 ppb), Cs (11 ppb), Hf (6 ppb), 
H+ (7 ppb) and a very low 0.8 ppb Ag are documented. The 99th percentile for Br (480 ppb) and the 98th percentiles for 
As (41 ppb) and Ga (15 ppb) are also present. The 100th percentile for specific conductance (28.8 mhos cm-1) is 
documented from this portion of the belt.

Further west, from the central portion of Sharpe Lake to the south end of Webber Lake, long and short strike length 
airborne and ground EM conductors are marked by base and precious metal enzyme leach signatures as well as 
numerous structurally-related elements. The 100th percentile values for Zn (73 ppb), Li (94 ppb – 2 responses), Sc 
(7841 ppb), Ti (2922 ppb), Rb (159 ppb), Sr (1803 ppb), Zr (148 ppb), Hf (6 ppb), I (226 ppb) and Br (598 ppb) are 
present. Additionally, 99th percentile responses for Mo (46 ppb, plus a 98th percentile response of 28 ppb) and Y (68 
ppb and a 67 ppb 98th percentile) and a 98th percentile for Pb (19 ppb) are documented. Also noteworthy are the 100th 
percentile specific conductance response (28.8 mhos cm-1) and the 98th percentile for H+ (4.7 ppb). A somewhat 
different metallogenetic environment is indicated by a cluster of 100th (32 ppb), 99th (27 ppb) and 98th (23 ppb) 
percentile Th responses associated with a 4 ppb U 99th percentile that extends north of west-central Sharpe Lake to 
Barclay Lake. This anomaly was also marked by conspicuous Sb-in-rock enrichment (63 ppb and 10 ppm) in two 
samples and is related to highly fractured, pyritic and “yellow stained” bleached rocks.

Further north to Barclay Lake, a 100th percentile Br response (598 ppb) and 98th percentiles for Y (67 ppb), Zr (93 ppb) 
and REE (513 ppb, also a 432 ppb 95th percentile response) characterize a small greenstone outlier centered on this 
lake. The west shore of the lake is marked by a round aeromagnetic response that appears to correlate to weakly 
mineralized (1% pyrite), carbonate-altered and epidotized diorite exposed at the west lake shore.


Synthesis

Enzyme leach based b-horizon soil geochemical survey results have effectively delineated multi-sample and multi-
element low to high contrast anomalies centered on the Little Stull Lake gold deposits in the Edmund Lake belt and the 
Twin Lakes and Seeber River gold deposits in the Sharpe Lake belt. The latter gold deposits are situated at or close to 
the contact between Oxford Lake Group volcanic and sedimentary rocks and this contact is marked by persistent 
single sample and linear east-west trending multi-sample responses. A similar response is noted in other areas of both 
belts where structural features such as the Edmund Lake portion of the Wolf Bay Shear Zone and the southern 
margins of the Sharpe Lake belt (south of Monument Bay and west to Twin Lakes near the Oxford Lake sedimentary 
and volcanic rock contact) are marked by high contrast responses of commodity or “ore and ore-related elements” as 
well as elements usually associated with faults and shear zones. These areas define potentially favourable exploration 
targets.

Significant multi-element enzyme leach soil geochemical anomalies were identified south of Makataysip Lake at or 
near the contact between Oxford Lake Group sedimentary rocks and Hayes River basalt in the Sharpe Lake belt, and 
southeast of the Little Stull Lake gold deposits to the Manitoba-Ontario provincial border in Edmund Lake belt. Both of 
these locations had been previously identified on the basis of the results of the rock geochemical survey.

Modest but consistent base and precious metal responses were obtained from samples collected in the Sharpe Lake 
area. Of particular interest in this part of the Sharpe Lake belt is the association of highly elevated Sb-in-rock and U 
and Th b-horizon soil signatures. These responses are associated with highly altered and mineralized felsic 
(bleached?) intrusions that are stained to varying degrees of intensity with a yellow coating reminiscent of uranium 
oxide. Further efforts to identify this mineral coating have not been undertaken. These rocks locally host up to 20% 
disseminated and veinlet pyrite and are exposed sporadically over approximately 4 km. The exposure of these 
mineralized rocks was the result of intense forest fires in this portion of the belt and the ability to land the helicopter for 
sampling in the same area. The association of U-Th-REE suggests the need to assess these mineralized zones for 
platinum group element contents. As of the writing of this report, PGE analyses have not been undertaken.

The nature of the b-horizon samples collected in 1997 shows a preponderance of variably oxidized glacial Lake 
Agassiz clays. These surficial deposits comprise 80% of the b-horizon soil samples collected in 1997 with the 
remainder represented by silt (6.4%), sand (4.5%), till (4.2%) and 4.9% of samples classified as “mixed” owing to the 
mixing of sands, silts, clays and tills by permafrost action. Within the body of anomalous responses identified in the 
1997 survey area, there is a lack of preferential development of high, medium or low contrast geochemical anomalies 
in any one particular b-horizon soil type. It is somewhat difficult to assess the effects of primary b-horizon soil 
composition on enzyme leach response given the preponderance of lacustrine clays as the sample media.

Noteworthy in this enzyme leach survey is the success of the technique at the 1 km sampling scale and the 
correspondence with the rock geochemical survey results.

Conclusions

The following conclusions are apparent from the 1997 b-horizon soil geochemical survey based on the enzyme leach 
process:

1)	known zones of gold mineralization and their respective stratigraphic structural rock “packages” have been 
effectively delineated;

2)	new zones of high contrast geochemical response have been delineated at or near the southern greenstone belt 
margins and are interpreted to represent fault structures with associated precious metal mineralization;

3)	the northern contact of the Oxford Lake Group Sedimentary and volcanic rocks, as well as the southern Oxford 
Lake Group sedimentary rock and Hayes River basalt contact is identified as highly prospective for precious metal 
mineralization. These contacts are sites of significant rheologic difference and as such are probably faulted or 
sheared. The association of “ore and ore-related” precious metal assemblages as well as elements usually 
observed in association with structural features (Sc, Nb) would tend to support this hypothesis;.

4)	a properly collected, prepared and analyzed b-horizon soil sample can effectively target base and precious metal 
targets for subsequent follow-up;

5)	the significant areal expanses of wet peatlands in the 1997 multi-media survey does not prohibit the acquisition of 
meaningful soil geochemical data derived from the enzyme leaching of b-horizon soil samples.



HUMUS GEOCHEMICAL SURVEY 
Sample Collection

Humus samples were collected from beneath the moss mat that was normally removed prior to digging the till sample 
pit. Where the humus layer was too thin or had become contaminated with inorganic sediment during the course of 
digging, the sample site was moved to a suitable location 5-10 m away from the till hole. The humus collected from 
these sites was generally moderately to well humified and had a fine grained, sooty consistency. Care was taken not 
to include inorganic material with this sample type. Enough humus was collected to fill a large ZIPLOC freezer bag. At 
some locations, the humus was a dark brown colour and less humified. In burned areas, humus was collected as 
residual mats off of boulders or from low-lying areas or small gullies where the temperatures associated with the fire 
had not been sufficiently high so as to ash the humus. Duplicate samples were collected at approximately every tenth 
site.

Sample Preparation and Analysis

Humus samples were air dried at room temperature on disposable plastic plates in the laboratories of the Manitoba 
Geological Services Branch. After drying, the samples were sieved and the -80 mesh size fraction retained. This 
sample was forwarded to Activation Laboratories Ltd. (Ancaster, Ontario) for INA and ICP-AES analysis. The ICP-AES 
analysis at Activation Laboratories Ltd. is based on a four acid total digestion. A second portion of the -80 mesh humus 
sample was submitted to the laboratories of the Manitoba Geological Services Branch for the measurement of pH and 
conductivity. The pH and conductivity measurements were corrected and converted to H+ and specific conductance 
using the formula of Govett (1976) and reproduced with examples in Govett et al., (1984).

Geochemical analyses are listed in Appendix 1 (ICP-AES, H+, K and Hg) and 4 (INA). Analyses for duplicate pairs are 
given in Appendices 2 (ICP-AES, H+, K and Hg) and 6 (INA). Percentile bubble plots are given in Appendices 3 (ICP-
AES, H+, K and Hg) and 5 (INA).

Results
	Edmund Lake Belt

Despite somewhat lower contrast in the geochemical responses of humus samples from this belt, the positions of 
known gold mineralization and geochemically anomalous areas delineated by rock and b-horizon soil geochemical 
surveys are identified. One area where humus geochemistry did not reproduce rock and soil anomalies occurs at the 
deflection of the Wolf Bay Shear Zone (WBSZ). A 99th percentile value of 0.76% Mg is documented from this site; no 
other significant humus geochemical responses were identified.

The most significant multi-element, multi-sample high contrast anomalies occur in the general area of Little Stull Lake, 
including the Little Stull Lake gold deposits, and in the area south and east of the lake to the Manitoba-Ontario 
provincial border. The Little Stull Lake gold deposits are marked by 100th percentile responses for Br (63 ppm), Ni (72 
ppm) and Ca (71%); a 99th percentile for U (8.8 ppm) and a 98th percentile As response (5 ppm) also occurs at these 
mineralized zones. The area just east of Ken Bay on Little Stull Lake is marked by significantly more anomalous 
responses than the known gold mineralization. This area is marked by 100th percentile values for Fe (3.86%), Cr (70 
ppm), Hf (7 ppm), Rb (81 ppm), Sc (24 ppm), Th (13 ppm), Zn (200 ppm by INAA and 160 ppm by ICP-AES), REE 
(189.4 ppm), Ni (31 ppm), V (123 ppm), Ti (0.37%), Al (7.19%), K (1.73%) and Y (24 ppm). Cu (99th percentile at 46 
ppm and 98th percentile at 40 ppm) and Co (98th percentile at 9 ppm) are also documented from this area. These 
responses may be attributed to the eastern extension of a previously unrecognized variably sheared and altered 
gabbro that contains a >1m thick sulphide zone situated on the north shore of Ken Bay (Corkery, 1997). Assay 
samples collected from this indicate low metal contents (T. Corkery, pers. comm.). 

Southeast of the Little Stull Lake gold deposits along the WBSZ, a 100th percentile value for As (5.9 ppm), Zn (200 
ppm) and Ba (570 ppm) are documented. West of the gold deposits the 100th percentile for REE (189.4 ppm), as well 
as the 99th and 98th percentiles for Ni (44 ppm and 25 ppm) respectively and Hf (6 ppm) as well as 99th percentiles for 
Co (10 ppm) and Y (20 ppm) are observed. The 98th percentile for Sr (130 ppm) occurs west of the northwest end of 
Little Stull Lake.

Southeast of Little Stull Lake in an area that has previously been defined as geochemically anomalous by rock and b-
horizon soil surveys, multiple significant base metal responses in humus are documented. Probable lithologic and 
alteration-related 100th percentile responses are recorded for Ni (72 ppm by INAA and 31 ppm by ICP-AES), Mg 
(1.25%), Ca (7.1% as well as two 98th percentile values of 5.81%), K (1.73%), Y (24 ppm) and Sr (159 ppm). Ninety-
ninth percentiles for Al (4.36% as well as a 98th percentile of 4.28%), REE (183.9 ppm), Rb (51 ppm plus a 98th 
percentile of 49 ppm), U (8.8 ppm) and Th (9.2 ppm and a 98th percentile of 6.9 ppm) are also recorded. Base metal 
signatures in the area are marked by 98th percentile values for Cu (40 ppm), Zn (117 ppm by INAA and 120 ppm by 
ICP-AES), Bi (7 ppm) as well as V (57 ppm), Mn (1564 ppm), Ti (0.19%) and Sc (8.3 ppm and a 95th percentile of 5 
ppm).

Some interesting high contrast responses are localized at the margin of the Edmund Lake belt, southwest of Little Stull 
Lake. In this area, probable faulting and/or shearing at the volcanic-intrusive contact, is marked by 100th percentile 
responses for As (5.9 ppm and a 99th percentile of 5.5 ppm), Hg (445 ppb as well as 99th and 98th percentiles of 377 
and 356 ppb, respectively), U (23 ppm), Sr (159 ppm) and Mn (2856 ppm). Ninety-eighth percentiles for Bi (7 ppm) 
and Ca (5.81%) are also present.

Humus geochemical results identify the peripheral area of the Margaret Lake granite intrusion as being marked by 
numerous anomalous responses. The southern area of the intrusion is marked by 100th percentile values for Mo (7 
ppm) and specific conductance (49 mhos cm-1; water-extractable metal) and 98th percentiles for Cr (39 ppm), REE 
(155.2 ppm) and Ti (0.19%). North and northeast of the intrusion 100th percentile responses for specific conductance 
(49 mhos cm-1), Rb (81 ppm) and Al (7.19%), 99th percentiles for K (1.16%), Ti (0.20% and a 0.19% 98th percentile), P 
(0.166%), V (62 ppm), Zn (128 ppm by INAA), Th (9.2 ppm), Sc (9.7 ppm) and Cr (44 ppm) are documented. A 98th 
percentile value for REE (155.2 ppm) is also present. The east end of the intrusion and related rocks is marked by a 
100th percentile concentration for Zn (200 ppm by INAA and 160 ppm by ICP-AES) and Mn (2856 ppm). Scattered 
about the periphery of the intrusion are clusters of 98th, 95th and 90th percentiles for Pb (34, 26 and 23 ppm, 
respectively) and 98th and 95th percentiles for specific conductance (33.7 and 30.2, respectively). The area at the west 
end of Margaret Lake is also anomalous with a 100th percentile response for H+ (139.16 mhos cm-1) and a 98th 
percentile for Pb (34 ppm). These responses reflect proximity to a magnetite-rich iron formation that outcrops in this 
area.

The Edmund Lake area at the western extremity of the belt is transected by the WBSZ and intruded by an earlier 
granitic intrusion in the central portion of the lake. This is the White House tonalite, a strongly foliated, fine to medium 
grained equigranular intrusion and a younger plagioclase porphyritic biotite tonalite (Corkery, 1997). Alteration of these 
units is restricted to epidotization of feldspars and biotite altered to chlorite. Humus geochemical responses from the 
Edmund Lake area includes the 100th percentile for Au (43 ppb) and P (0.183%), 98th percentile for U (6.2 ppm) and 
the 95th percentile for Cr (32 ppm), all of which occur on the west shore of the lake. The islands in the central portion of 
the lake are marked by a 100th percentile value for P (0.183%), 98th percentile for U (6.2 ppm) and H+ (85.1 ppb as well 
as a cluster of three 95th percentiles of 75.6 ppb). The east shore, in proximity to the WBSZ has a 99th percentile 
response for specific conductance (35.3 mhos cm-1) and a 98th percentile for Zn (118 ppm). A 98th percentile response 
for Bi (7 ppm) is reported from the south portion of the lake.

Two final areas in the Edmund Lake greenstone belt are noteworthy for their moderately high contrast humus 
geochemical responses. These areas occur on Rorke Lake near the Manitoba-Ontario provincial boundary and on the 
west shore of Kistigan Lake. The north Rorke Lake area is marked by 100th percentiles for Cu (82 ppm – 2 responses), 
Co (21 ppm), Fe (3.86%) and V (123 ppm) and 99th percentile responses for Cr (44 ppm), Sc (9.7 ppm) and Hf (6 
ppm). The Fe, V and Cr responses are probably attributable to an occurrence of high-Mg volcanic flows (komatiite?) 
documented on the north shore of Rorke Lake by Corkery (1997a). A deformation zone occurs to the north of this unit. 
The west shore of Kistigan Lake has 100th percentile values for Mg (1.25%) and Ti (0.37%) and 98th percentiles for Bi 
(7 ppm – 2 responses) and H+ (85.1 ppb). A 99th H+ response (87.1 ppb) occurs west of Kistigan Lake midway to 
Margaret Lake.


	Sharpe Lake Belt

Significant humus geochemical responses were also obtained from sites within the Sharpe Lake belt that were 
previously deemed “anomalous” by rock and b-horizon soil surveys. Interestingly, exceptions appear to be the Twin 
Lakes area (site of the Twin Lakes and Seeber River gold deposits) and a very limited response on the west shore of 
Makataysip Lake where 98th percentile values for Cu (22 ppm) and specific conductance (30.86 mhos cm-1) were 
obtained. The Makataysip Lake area is marked by a circular 6700nT aeromagnetic anomaly that has multiple rock and 
b-horizon soil geochemical responses associated with it.

The Monument Bay area contains multiple high contrast geochemical responses that are concentrated primarily at the 
north end of the lake, at or near the contact between the Oxford Lake Group volcanic on the north and the 
sedimentary subgroup on the south. This contact localizes gold mineralization at the Twin Lakes and Seeber River 
gold deposits and is undoubtedly faulted and/or sheared. The area is characterized by 100th percentile values for Pb 
(29 ppm), REE (169.4 ppm and a 98th percentile of 125.7 ppm), Rb (44 ppm) and two specific conductance responses 
of 47.39 mhos cm-1 and 99th percentiles for Cu (26 ppm and a 98th percentile response of 22 ppm), Au (8 ppb), Ni (20 
ppm), Bi (8 ppm – 3 responses and a 7 ppm 98th percentile), Mn (901 ppm) and Y (16 ppm). It is noteworthy that the Bi 
responses trend southwards to the Manitoba-Ontario provincial border from the north end of Monument Bay. 
Additionally, 98th percentile values for Zn (93 ppm by INA and 58 ppm by ICP-AES), Fe (1.58%), Cr (37 ppm), Co (7 
ppm), Br (33 ppm), V (34 ppm), Hg (356 ppb), Th (6.5 ppm), and U (6.6 ppm and a 95th percentile of 4 ppm). The U 
response appears to track westward towards Twin Lakes along the volcanic-sedimentary contact. A 98th percentile 
response for Ni (72 ppm) is also noted from the south end of Monument Bay.

The area south of Monument Bay comprises another east-west geological contact that is probably faulted. The contact 
occurs at the south end of Monument Bay where Hayes River basalts (south) are in contact with Oxford Lake Group 
sedimentary rocks to the north. This contact and the Hayes River basalts to the south are marked by 100th percentile 
values for Ni (57 ppm), Co (27 ppm), Fe (3.6% and two 98th percentile responses of 1.58%), Sc (13 ppm and a 98th 
percentile of 4.8 ppm), V (111 ppm), Ti (0.46%), Al (5.09% and two 98th percentiles of 3.49%), Na (1.35%) and Mg 
(0.95% with 99th and 98th percentile values of 0.61 and 0.57%, respectively). Ninety-ninth percentile responses include 
Zn (61 ppm), Cu (26 ppm), Th (6.8 ppm), K (0.78%) and Hf (5 ppm). The 98th percentile responses documented from 
the area are Cr (37 ppm), Mn (680 ppm), Y (13 ppm) and H+ (79.2 ppb).

Despite the relative paucity of anomalous responses in proximity to the Twin Lakes area, south of the lakes, multiple 
high contrast responses are documented from samples collected over the Oxford Lake Group sedimentary rocks and 
their east-west contact with granitic intrusions at the southern margin of the belt. The southern margin of the belt is 
marked by a 100th percentile value for Ca (5.81%), a 99th percentile for Co (8 ppm) and a 98th percentile V response of 
34 ppm. This modest geochemical response is significant in that it is suggestive of the need for more Fe-rich rocks, 
such as the Hayes River or Oxford Lake Group basalts, to react (reduce) with hydrothermal fluids that may be using 
the faulted contact as a plumbing system. Within the Oxford Lake Group sedimentary rocks, multiple responses are 
obtained but appear to be restricted to lithologically or structurally-related elements. These include 100th percentile 
values for K (1.22%), Sr (182 ppm), Na (1.35% and 99th and 98th percentiles of 0.94 and 0.9%, respectively), REE 
(169.4 ppm), Hf (6 ppm) and H+ (123.9 ppb). Ni responses may be indicative of a mineralized zone or of a high-Mg 
lithology. It is measured as a 100th, 99th and 98th percentile (89, 75 and 72 ppm, respectively) in this area. Ninety-ninth 
and 98th percentiles are also present for Ba (2 responses, 400 ppm), Rb (38 ppm) and Ti (0.19%), U (6.8 ppm) and Sc 
(4.8 ppm), respectively. West of the south end of Twin Lakes is a 99th percentile response for Y (16 ppm). A 99th 
percentile for P (0.186%) and a 98th percentile for Mn (680 ppm) are noted mid-way to southern Makataysip Lake.

The area south of Makataysip Lake is marked by two geological contacts. West and south of the lakeshore in the 
Oxford Lake Group sedimentary rock contact with Hayes River basalts. Further south is the contact of the Hayes River 
basalts and the granitic intrusive rocks. The southernmost Hayes River basalt/granite contact just west of the south 
end of Makataysip Lake is marked by 100th percentile values for Ni (57 ppm), Ti (0.46%), Al (5.09%), Y (24 ppm), Mn 
(2065) and H+ (123.9 ppb and a 98th percentile of (79.2 ppb). A 99th percentile for V (75 ppm) and a 95th percentile for 
Pb (22 ppm) also characterize this area. In the area immediately south of Makataysip Lake, which includes the 
sediment-volcanic rock contact 100th percentile values for Au (28 ppb and a 99th percentile of 8 ppb), As (1300 ppm 
and 99th and 98th percentile values of 38 ppm and 7.7 ppm, respectively) are documented. The 1300 ppm analysis 
represents the highest As measured in humus in the 1997 survey. Additional 100th percentiles include Co (27 ppm), Cr 
(50 ppm and a 99th percentile of 40 ppm), Fe (3.6%), Sc (13 ppm), Th (13 ppm), Ca (5.81% and a 99th percentile of 
5.65%) and Cu (130 ppm). Ninety-ninth percentile responses for REE (129.7 ppm) and Ba (37 ppm and a 98th 
percentile of 33 ppm) and 98th percentiles for Mo (2 responses, 9 ppm), Na (0.94%) and Hf (4 ppm) are also 
documented. A 99th percentile for H+ (85.1 ppb) occurs east of the south end of Makataysip Lake as well as a 100th 
percentile response for Ba (63 ppm). West of the south end of the lake, a 99th percentile value for REE (129.7 ppm) 
and a 98th percentile for Na (0.94%) are documented. The area west of Makataysip Lake is geologically characterized 
by Hayes River basaltic and chemical sedimentary rocks.

The east Sharpe Lake area contains 100th percentile values for Hg (445 ppb and 99th and 98th percentiles of 377 and 
356, respectively), U (15 ppm), P (0.207%) and Rb (44 ppm). A 99th percentile response of 10 ppm for Mo and 98th 
percentiles for Zn (93 ppm) and Pb (22 ppm) are also documented.

The west-central portion of Sharpe Lake, including southern Webber Lake is marked by moderate to high contrast 
base and precious metal anomalies. One hundredth percentile values for Mo (19 ppm and a 98th percentile of 9 ppm), 
U (15 ppm), Zn (2 responses at 167 ppm and a 98th percentile of 93 ppm), Pb (29 ppm), Mn (2065 ppm), P (0.207%), 
Mg (0.95%), Ba (430 ppm and a 98th percentile of 350 ppm), Br (47 ppm) and K (1.22%) are documented. The 99th 
percentile responses include Fe (1.9%), Cr (40 ppm), As (38 ppm), Sc (5.4 ppm) and specific conductance (32.66 
mhos cm-1). Ninety-eight percentile values were obtained for REE (125.7 ppm), Na (0.9%) and Ni (72 ppm). A 100th 
percentile for Al (4.13%) and Sr (182 ppm) were obtained from samples south of Webber Lake.

The small area of greenstone centered on Barclay Lake and marked by a small aeromagnetic anomaly on its west 
shore is characterized by a 99th percentile response for Mo (10 ppm) southwest of the lake. Ninety-eighth percentile 
values for U (6.6 ppm) and Zn (93 ppm) were also documented. The area of the aeromagnetic response is 
characterized by weakly mineralized (1% pyrite) carbonate-altered and locally epidotized diorite.

Synthesis

Humus geochemical survey results for the Edmund Lake and Sharpe Lake greenstone belts have successfully 
identified regional metallogenetic features associated with known structural, lithological and stratigraphic associations 
for both base and precious metals. The WBSZ in the Edmund Lake belt is confirmed as a highly prospective precious 
metal target. It’s importance is demonstrated by the fact that out of 9 Au analyses (INAA) above the lower limit of 
detection in humus samples collected over the Edmund Lake belt, 7 of these were from samples collected over the 
WBSZ. The 100th percentile response for Au (43 ppb) in the belt occurs at the west end of the WBSZ at Edmund Lake, 
while the Little Stull Lake gold deposits are situated within the eastern portions of this regional structural feature. These 
gold deposits have high contrast, multi-element and multi-sample humus geochemical responses. The area east and 
south of the gold mineralization is identified as a high priority area for exploration follow-up based on multiple 
geochemical anomalies revealed by the humus survey. Of some interest is the apparent lack of geochemical response 
in humus samples collected in proximity to the WBSZ deflection. Rock and b-horizon soil samples collected in the area 
of the deflection illustrated base and precious metal responses. The observation of multiple geochemical responses 
peripheral to the Margaret Lake granite intrusion in rock and b-horizon soil samples is re-confirmed by the humus 
survey results, including an obvious pattern of elevated specific conductance in samples from the vicinity of the 
contact between the mineralized granite intrusion and basaltic country rocks.

The coincidence between a possible komatiite occurrence on the north shore of Rorke Lake and the coincident 
anomalies for Cu, Co, Fe, V, and Cr indicate the successful recognition of “unique” lithologies by the sampling media. 
The gold mineralization at Ken Bay (Little Stull Lake) in association with altered gabbros would be another example of 
the positive correlation between humus geochemistry and unique lithologies. 

The results of the humus geochemical survey in the Sharpe Lake belt has been equally successful with one exception. 
This is the absence of any significant geochemical response in association with the Twin Lakes and Seeber River gold 
deposits. It is curious that the Oxford Lake Group sediment-volcanic contact that localizes the gold mineralization in 
the Twin Lakes area is highly geochemically anomalous between Twin Lakes and Monument Bay but geochemically 
“flat” over the deposits. The sheared and altered contact, however, is pinpointed as a highly prospective exploration 
target as is the Oxford Lake Group sedimentary subgroup – Hayes River basalt contact south of Monument Bay and 
west to Makataysip Lake. In fact, the geochemical responses from the Makataysip Lake area (including a 1300 ppm 
As analysis) are amongst the most significant in rock, till, b-horizon soil and humus surveys conducted in 1997. 
Conversely, the Oxford Lake Group sedimentary – granite contact at the southern margin of the Sharpe Lake belt has 
few commodity-related responses. It is postulated that the absence of Fe-rich rocks (basalt/iron formation) at this 
sheared contact precludes hydrothermal mineralization. This contact with Hayes River basalts to the east and west is 
marked by multiple geochemical responses.

The western portion of the Sharpe Lake belt is inferred to have a somewhat different metallogenetic signature based 
on the humus geochemical survey results. In this part of the belt, base metal and U-REE signatures appear to 
predominate over those for precious metals, although this may simply be a function of sample distribution. A U-REE-
Sb association has been documented in humus samples collected in proximity to a bleached, fractured, pyritic and 
yellow stained felsic intrusions that occur on the north shore of central Sharpe Lake. These highly altered are exposed 
over 4-5 km in an east-west zone exposed by intense forest fires. Platinum group element analyses should be 
undertaken on these samples.

Despite its small areal distribution the greenstone outlier at Barclay Lake should be examined closely on the basis of 
its circular aeromagnetic anomaly on the west shore, the altered mafic intrusive rocks exposed sporadically along the 
lakeshore and its Mo, U and Zn geochemical responses.

Conclusions

The results of this humus geochemical survey in the Edmund Lake and Sharpe Lake greenstone belts indicate the 
following:

1)	humus geochemical surveys undertaken at approximately 1 km sample spacing have successfully delineated 
known gold deposits and their associated stratigraphic structural rock “packages”;

2)	the exceptions to 1) are the Twin Lakes and Seeber River gold deposits;

3)	regional metallogenetic features such as the WBSZ and Oxford Lake Group sediment – volcanic contact are 
identified as highly prospective targets for precious metals;

4)	the area south and west of Makataysip Lake displays exceptional geochemical relief in terms of the high contrast, 
multi-element and multi-sample of the anomalies;

5)	geochemical anomalies peripheral to the Margaret Lake intrusion are established on the basis of humus 
geochemistry, particularly water-extractable metals as measured by specific conductance;

6)	elevated specific conductance measurements usually coincide with elevated metal contents in humus;

7)	an U-REE-Sb association in highly altered felsic intrusions exposed as a result of an intense forest fire in central 
Sharpe Lake is recognized and analysis of samples from this zone for platinum group elements is warranted.


VEGETATION GEOCHEMICAL SURVEY 

Introduction

Unlike the 1996 survey, only vegetation crown twigs were sampled and analysed. This modification to the sampling 
plan was instituted due to higher contrast geochemical response for most elements in the crown twigs. Data 
interpretation proceeds from the Edmund Lake belt to the Sharpe Lake belt; results for INAA and ICP-AES are 
integrated for purposes of discussion.

It should be noted that unlike rocks, soils, lake sediments and other types of geochemical sample media, trees and 
other plants have certain nutrient requirements in order to survive. This effectively divides elements into essential and 
non-essential categories. For these reasons, the essential element Zn, which is necessary for plant metabolism, must 
be interpreted with caution since subtle variations in the Zn concentrations of vegetation samples from site to site may 
only reflect the general state of the health of the tree. Major differences may indicate the presence of mineralization 
containing Zn or a Zn-enriched substrate. Tables 1 and 2 summarize essential and non-essential elements and their 
role in plant function.

Sample Collection

Samples of twigs from the crowns of black spruce (Picea mariana) were collected from each sampling site. Sampling 
was undertaken over an 8-week period between June and August, 1997. At most sites, the vegetation samples were 
collected from within 20m of the till sampling pit. Black spruce was selected as the target sampling medium on the 
basis of its ubiquitous presence throughout the survey area and for its usefulness in delineating metal-enriched 
substrates in other vegetation geochemical surveys (Fedikow and Dunn, 1996).

Black spruce crown twigs were obtained by cutting down the tree and collecting the upper 45 cm of the tree using 
anvil-type pruning shears. These samples were stored in labelled, brown paper bags and allowed to dry before 
preparation. A thin 2-3 cm wafer was cut from each tree for age dating and for comparisons between element content 
and tree age.

Sample Preparation and Analysis

Subsequent to drying, the needles and cones were removed from the crown twigs and stored separately for future 
study. For twig samples, approximately 50g of material was weighed into aluminum trays and the trays placed into a 
pottery kiln. The kiln temperature was raised incrementally over a 2-3 hour time period to a maximum of 470oC. This 
temperature was maintained for 12 hours at which time the vegetation had been reduced to about 1g of ash without 
charcoal. One half of this ash was accurately weighed into polyethylene vials and submitted for instrumental neutron 
activation analysis. The second half of the ash was submitted for ICP-AES analysis subsequent to an aqua regia 
dissolution. Both analytical approaches to vegetation ashes were undertaken at Activation Laboratories Ltd. (Ancaster, 
Ontario). The aqua regia dissolution is a total digestion for most metals but is only partial for some elements such as 
Ni and Zn. The element distribution patterns for elements that are only partially taken into solution by the aqua regia 
digest are considered to be valid since analytical precision for most elements is acceptable.

Geochemical data is presented in Appendices 1 (ICP-AES) and 4 (INAA); duplicate pair geochemical data is given in 
Appendices 2 (ICP-AES) and 5 (INAA). Percentile bubble plots are presented in Appendices 3 (ICP-AES) and 6 
(INAA).


Table 1.	Essential and non-essential elements determined by INAA.

Element
Essential/Non-Essential/Comments
Au
Non-essential
Ag
Non-essential
As
Essential/metabolism of carbohydrates
Ba
Non-essential
Br
Non-essential
Ca
Essential/cell wall construction
Co
Essential/major nutrient fixation
Cr
Non-essential
Cs
Non-essential
Fe
Essential/photosynthesis, chlorophyll
Hf
Non-essential
K
Essential/metabolism
Mo
Essential
Na
Non-essential
Rb 
Essential
Sb
Non-essential
Sc
Non-essential
Se
Essential
Sn
Non-essential
Sr
Essential
Ta
Non-essential
Th
Non-essential
U
Non-essential
W
Non-essential
Zn
Essential/carbohydrate and protein metabolism
REE
Non-essential


Table 2. Essential and non-essential elements determined by ICP-AES

Element
Essential/Non-Essential/Comment
Al
Non-essential
B
Essential/plant growth, sugar translocation
Be
Non-essential
Cd
Non-essential
Cu
Essential/respiration, photosynthesis
Li
Essential/metabolism
Mg
Essential/photosynthesis, enzyme reaction
Mn
Essential
Ni
Non-essential
P
Essential/energy metabolism
Pb
Essential in small amounts/cell walls (?)
Ti
Essential/photosynthesis
V
Non-essential


Results
	Ash

Ash contents in black spruce crown twigs is similar for both the Edmund Lake and Sharpe Lake greenstone belts. Ash 
contents vary between 1.72 – 2.34% and 1.77 – 2.79%, respectively. Interestingly, the highest ash contents coincide 
with some of the areas of high vegetation metal contents that are also reflected by other sampling media. Examples 
are in the areas southeast of Little Stull Lake near the Manitoba-Ontario provincial border and on the east shore of 
Edmund Lake in the Edmund Lake belt and from the Monument Bay and west Sharpe Lake areas in the Sharpe Lake 
belt.

	Edmund Lake Belt

Vegetation geochemical results along the belt vary from multi- to single sample, high to moderate contrast multi-
element responses that successfully delineate the location of known mineral deposits, regional structures such as the 
Wolf Bay Shear Zone (WBSZ) and unique lithologies. The Little Stull Lake area, including the gold deposits on the 
southwest shore of the lake, is an excellent example of the usefulness of the vegetation geochemical approach. The 
area is marked by 100th percentile values for As (3.8 ppm), Ba (2800 ppm), Pb (64 ppm) and a 98th percentile value of 
3500 ppm Zn just west of the deposits. The 100th and 99th percentile values for Zn (4300 ppm and 3600 ppm, 
respectively) and the 99th and 98th percentile values of 1500 ppm and 1400 ppm, respectively, are documented from 
the Ken Bay area as well as east and west of the Little Stull Lake gold deposits. Additional responses include the 100th 
percentile value of 4300 ppm for Sr east of the deposits and a 100th percentile value of 14 ppm Sb northwest of the 
deposits along the WBSZ. Northeast of the deposits on the east shore of Little Stull Lake 100th and 99th percentile 
values for Cr (28 ppm and 20 ppm, respectively) are documented. The 100th, 99th and 98th percentile values for Na 
(3870 ppm, 3380 ppm and 3310 ppm, respectively) occur directly over the Little Stull Lake deposits as well as a 100th 
percentile value of 0.93% Fe. The north and northwest shores of Little Stull Lake are marked by 100th percentile values 
for Fe (0.62%), V (12 ppm, as well as 98th percentiles of 10 ppm both east and west of the 100th percentile), REE (42.8 
ppm, and a 99th percentile of 29.4 ppm just west of the gold deposits along the WBSZ) and Hf (1.5 ppm). An Al 
response of 0.58% (99th percentile) must be viewed with caution since twig over the Little Stull Lake deposits as well 
as a 100th percentile value of 0.93% Fe. The north and samples were ashed in aluminum trays and some Al 
contamination could have affected the samples during preparation. A 99th percentile value for Sc (2.2 ppm) at the north 
end of Little Stull Lake as well as a 99th percentile response for Zn (2894 ppm) on the northeast shore and a 98th 
percentile value for K (13.85%) on the north shore are documented. A 100th percentile value for Pb (64 ppm) and Cr 
(21 ppm) occurs on the east and southeast shores of the lake, respectively. A 98th percentile response for Br (66 ppm) 
occurs at the Little Stull Lake gold deposits.

Southeast of the Little Stull Lake area to the Manitoba-Ontario border is an area of significant precious and base metal 
signatures, as well as responses that could be attributed to unique lithologies such as high-Mg basalt or ultramafic 
rocks. Base metal signatures are reflected by 99th percentile values for Pb (3 responses – 37 ppm) and Ni (156 ppm), 
and 98th percentile values for Fe (clustered at 0.67%), and Cu (378 ppm). Precious metal responses are documented 
for Au (99th and 98th percentiles of 27 and 25 ppb, respectively), Sb (99th percentile of 10 ppm) and As (98th percentile 
of 2.9 ppm). A high-Mg lithology is suggested by 100th and 99th percentile responses for Mg (7.64% and 7.16%, 
respectively), 99th and 98th percentiles for Cr (16 and 12 ppm, respectively) and two 98th percentiles for V (10 ppm). 
Alteration accompanying base and/or precious metal mineralization or a primary source of rare earth elements may be 
reflected by 98th percentile values for REE (25.3 ppm), Ba (374 ppm), Zr (7 ppm), Sc (2.1 ppm and a 95th percentile of 
1.7 ppm) and Al (2 responses – 0.51%, contamination?). Ninety-eighth and 95th percentile values of 13.85% and 
13.24% K, respectively may be indicators of the relative health of the tree (metal-induced stress?) since K is an 
element essential to metabolism.

Southwest of Little Stull Lake at the belt margin where faulting may characterize the contact between basaltic volcanic 
rocks and the granitic intrusive terrane, a strong precious metal response is documented. This vegetation geochemical 
signature is characterized by a 100th percentile value for Au (65 ppb), 99th percentiles for As (3.2 ppm), and Mn (30854 
ppm, as well as a 98th percentile of 28837 ppm), and 98th percentiles for REE (25.3 ppm), Fe (0.58%) and Rb (750 
ppm). A 95th percentile for Sb (7 ppm) and a 90th percentile for Sr (808 ppm) are also documented at the contact. It is 
noteworthy that the contact southwest of Little Stull Lake is parallel to the regional trend of the WBSZ.

The deflection point of the WBSZ that occurs approximately midway between the northwest end of Little Stull Lake and 
Margaret Lake has been hypothesized as representing a dilational zone produced by dextral movement along the 
WBSZ. The general area of the deflection is marked by moderate contrast precious metal and related responses. In 
this general area, 100th percentile values for Sb (2.6 ppm), Rb (870 ppm) and Cs (78 ppm), 98th percentile responses 
for Au (25 ppb), Ba (2200 ppm), Fe (0.67%), K (13.85%) and a cluster of 98th percentile responses (66 ppm) and 95th 
percentiles (59 ppm) for Br. The association of anomalous Br with Au has been documented in previous vegetation 
geochemical surveys in Saskatchewan and Manitoba. West of the deflection along the WBSZ, a 98th percentile value 
for Ni (147 ppm) is observed. A 100th percentile for K (31.9%) occurs southeast of the deflection and a 99th percentile 
(29.5%) is documented to the northwest. Southeast of the deflection along the WBSZ, a 99th percentile K response of 
15.2% as well as a 98th percentile value for Ni (110 ppm) is observed. West and southwest of the deflection, at or near 
the belt margin a 98th percentile response for As  (2.9 ppm) and Sr (808 ppm) and a 95th percentile for Sb (7 ppm) are 
documented.

The general area of the periphery of the altered and mineralized Margaret Lake granite intrusion has been recognized 
as conspicuous on the basis of the 1997 multimedia geochemical survey results and these observations have been re-
affirmed by vegetation geochemical signatures. Moreover, significant regional differences are present in the 
distribution of elements such as Rb and Cs in proximity to the intrusion, when compared to the southeast end of the 
belt near Little Stull Lake. In the Margaret Lake area, multiple 99th (52 ppm) and 98th (37 ppm) percentile Cs responses 
are observed, as well as 100th (870 ppm), 99th (760 ppm) and 98th percentile values for Rb. These responses are 
clustered about the Margaret Lake intrusion, whereas to the southeast in the Little Stull Lake area geochemical flux is 
essentially nil. Ni responses about the intrusion are marked by 100th (230 ppm), 99th (130 ppm), and 98th (110 ppm) 
percentile values. Anomalous peripheral geochemical percentile responses are also observed for Au (98th – 25 ppb), 
Br (100th – 71 ppm), Fe (98th – 0.67%; 95th – 0.61%), Cu (100th – 460 ppm; 99th – 388 ppm), Mo (100th – 5.5 ppm; 99th 
– 4 ppm; 98th – 3 ppm), Cd (98th – 3.6 ppm), Ag (100th – 1.1 ppm), Sr (100th – 2800 ppm; 99th – 972 ppm), Mn (100th – 
31996 ppm; 98th – 28837 ppm), Ba (100th – 650 ppm; 98th – 374 ppm), Mg (100th – 7.64%), P. (100th – 21667 ppm; 98th 
– 20974 ppm), V (98th – 10 ppm), Zr (98th – 7 ppm), K (13.85%) and a cluster of 100th and 99th percentile Sb responses 
(2.6 and 1-2 ppm, respectively distributed between the WBSZ deflection and the Margaret Lake intrusion. 
Approximately 3 km southeast of the intrusion a 100th percentile value for REE (42.8 ppm) is documented and 5 km 
southeast is the 100th percentile response for Zn (3539 ppm). A 100th percentile Cd response of 6 ppm occurs south of 
the intrusion along the WBSZ. Additional responses include a cluster of Ba anomalies that extends south of the east 
end of the margin of the intrusion to the belt margin on the east that is marked by 100th (2800 ppm), 99th (2300 ppm) 
and 98th (2200 ppm) percentiles. At the east end of the intrusion is a northeast-southwest trend of 100th (69 ppm), 99th 
(20 ppm), 98th (17 ppm) and 95th (12 ppm) Co percentile values. At the intrusions west end the 99th percentile for Na 
(3380 ppm) occurs along the WBSZ. The magnetite-rich iron formation exposed in outcrop at the west end of Margaret 
Lake is marked by a 98th percentile value for P (20974 ppm).

The Edmund Lake area is characterized by anomalous responses for base-and precious metals as well as unique 
high-Mg lithologies. The precious metal signature is reflected by a 98th percentile value for Au (25 ppb) associated with 
a 98th percentile for Ba (2200 ppm) on the southeast shore south of the WBSZ, as well as a 95th percentile for Sb (7 
ppm) from the south shore. A strong Cu signature consisting of a 100th percentile response (460 ppm) from the central 
portion of the lake, and two 98th percentiles (378 ppm) from the east side of the lake, a 98th percentile for Mo (3 ppm) 
from the south shore and a 98th percentile for Ni (110 ppm) from the west shore characterize the base metal 
responses. Geochemical responses that may be attributed to high-Mg sources include 98th percentile values for Cr (16 
ppm – west shore), Mg (7.12% - central islands) as well as 100th (21667 ppm – central islands) and 98th (west shore – 
20974 ppm; east shore – 20974 ppm) percentile values for P. The west shore of Edmund Lake is also characterized 
by 100th percentile responses for Ca (40.2%) and K (18.84%) and a 99th and 98th percentile for Cs (52 and 37 ppm, 
respectively). The south shore is marked by a 100th percentile for Ca (40.2%) and a 98th percentile for Ba (374 ppm) 
whereas the central islands in Edmund Lake have 98th percentiles for Mg (7.12%) and Na (0.20%). A 100th percentile 
value for Mn (31996 ppm) is documented from the east shore of Edmund Lake at the WBSZ.

Other areas of anomalous vegetation geochemical responses include those of Rorke Lake and Kistigan Lake. The 
northwest shore of Rorke Lake is characterized by 100th percentile values for Au (65 ppb), Ag (1.1 ppm) and Zr (8 
ppm), 99th percentiles for Al (0.52% - contamination?) and Sc (2.2 ppm), and a 10 ppm 98th percentile for V. The west 
shore of Rorke Lake near the Manitoba-Ontario border has a 99th percentile Ba response of 388 ppm.

The west end of Kistigan Lake is also marked by an interesting geochemical response consisting of 100th percentile 
values for Mo (5.5 ppm) and Sb (14 ppm) and a 99th percentile value for Ba (388 ppm).

Midway between Kistigan Lake and Margaret Lake in an area geologically characterized by Hayes River basalts 
intruded by an apophysis of Margaret Lake granite, a significant base metal and possible high-Mg lithologic response 
was documented. A 100th percentile response was obtained for Zn (4300 ppm), Cd (6 ppm), Fe (0.93%), Hf (1.5 ppm) 
and Cr (28 ppm) as well as 99th percentile values for Pb (44 ppm), Sc (2.2 ppm) and All (0.52% - contamination?). 
These responses are restricted to a couple of sampling sites in this area.

	Sharpe Lake Belt

Multiple vegetation geochemical anomalies are documented from known mineralized zones (Twin Lakes and Seeber 
River gold deposits), distinctive geophysical responses and unique lithologies in the Sharpe Lake belt. Excellent 
coincidence between the vegetation responses and those defined by rock, till, b-horizon soil and humus geochemical 
surveys is observed.

The Monument Bay area, including the north shore at or near the Oxford Lake Group sedimentary-volcanic subgroup 
contact, as well as the south and west shores are marked by multiple, high contrast geochemical signatures. The base 
metal response at the north end of the lake is marked by significant percentile responses for Zn (99th – 4700 ppm, 98th 
– 3300 ppm), Cu (4 responses, 95th – 271 ppm), Pb (98th – 26 ppm), Co (98th – 10 ppm, 95th – 8 ppm) and Ni (99th – 
100 ppm, 98th – 2 responses, 93 ppm). Precious metal responses include Au (95th – 2 responses, 17 ppb) and Sb (98th 
– 2 responses, 6 ppm and 95th – 5.5 ppm). Other significant responses at the north end of Monument Bay including 
those that delineate this stratigraphic contact are Ba (100th – 2300 ppm, 98th – 2100 ppm); Rb (100th – 1200 ppm), Al 
(98th – 0.5%; contamination?), Mn (99th – 30970 ppm), Zr (99th – 8 ppm). The sedimentary-volcanic contact that marks 
the location of significant gold mineralization in the Twin Lakes area can be traced westward from the north end of 
Monument Bay to southern Twin Lakes on the basis of the percentiles for Br (100th – 68 ppm, 99th – 65 ppm, 98th – 63 
ppm), K (100th – 35.1%, 98th – 3 responses, 28.35%), Na (100th – 2900 ppm, 99th – 2250 ppm, 98th – 2230 ppm) and Sr 
(100th – 2 responses, 1150 ppm, 95th – 3 responses, 828 ppm).

South of Monument Bay to the Manitoba-Ontario border is another area of base-precious metal response. This 
includes a 100th percentile value for Au (214 ppb) and two 98th percentiles for Sb (0.9 ppm albeit at low concentration 
levels) as well as a base metal association of high percentiles for Cu (100th – 352 ppm) Zn (98th – 3300 ppm) and Fe 
(98th – 0.44%). A 98th percentile for Sr (898 ppm) is also documented from this area. Perhaps the most significant 
response in terms of delineating highly prospective areas is the response obtained for K. Elevated K signatures are 
localized at the contact between Oxford Lake Group sedimentary rocks and Hayes River basalts as well as the contact 
between the sedimentary subgroup and the granitic intrusive rocks. The anomalies trend westward to southern 
Makataysip Lake and are marked by 99th (28.9%), 98th (28.35%) and 95th (26.40%) percentiles. This trend is similar to 
that for the gold mineralized Oxford Lake Group sedimentary-volcanic subgroup in the north. 

The Twin Lakes area is marked by a significant precious metal assemblage in the area of the known gold 
mineralization but also westward along the Oxford Lake Group sedimentary-volcanic contact. The significant elevated 
percentile responses include Au (99th – 32 ppb), As (99th – 4 ppm), Co (98th – 10 ppm), Cs (95th – 15 ppm), Sb (99th – 
7.5 ppm, 95th – 5.5 ppm), Sr (100th – 1600 ppm, 99th – 1400 ppm) and a 98th percentile for Cr (14 ppm).

The area south of Twin Lakes is also marked by multiple base and precious metal responses in crown twig samples. 
These responses may be reflecting mineralized east-west trending structures, an unrecognized sedimentary-volcanic 
contact or the probable sheared south margin of the belt (sedimentary-granite contact) and associated mineralization. 
These responses include elevated percentiles for Au (98th – 30 ppb, 95th – 2 responses, 20 ppb), As (99th – 4 ppm, 98th 
– 2 responses, 3.8 ppm, 95th – 3.4 ppm), Sb (99th – 1 ppm) and a low 99th percentile of 1.2 ppm for Ag. Base metal 
signatures include Zn (100th – 4700 ppm, 95th – 2 responses 2900 ppm), Cu (98th – 284 ppm), Pb (100th – 36 ppm), Mo 
(100th – 20 ppm, 98th – 2.5 ppm) and Fe (100th – 0.78%, 98th – 0.52%). Other significant associated responses include 
elevated percentiles for REE (100th – 28.9 ppm), Cs (100th – 37 ppm, 98th – 22 ppm), Sc (100th – 2.1 ppm, 98th – 1.4 
ppm), Rb (98th – 2 responses, 780 ppm, 95th – 640 ppm), Ba (98th – 2 responses, 2100 ppm), Mn (100th – 34296 ppm, 
98th – 30798 ppm), Cr (99th – 17 ppm), V (100th – 12 ppm, 98th – 10 p ppm), Zr (99th – 2 responses, 8 ppm), Mg (99th – 
7.86%), Na (98th – 2 responses, 0.10%) and Al (100th – 0.64%, 98th – 0.5%, 95th – 2 responses 0.46%; contamination 
from ashing tray?).

The west shore of Makataysip Lake is marked by a circular 6700 nT aeromagnetic anomaly that is marked by a 100th 
percentile response for Ni (120 ppm) and a 95th percentile for Fe (0.45%) as well as elevated percentiles for Al (99th – 
0.52%), 98th percentiles for Na (0.10%), Br (2 responses, 63 ppm) and Ca (28.3%). A 95th percentile for Cs (15 ppm) 
was also documented in this area.

The area south and west of Makataysip Lake is characterized geologically by the contact between the Oxford Lake 
Group sedimentary subgroup and the Hayes River basalt and the Hayes River basalt – granite contact. Consistent 
with the Oxford Lake Group sedimentary – volcanic contact and the contact with granites at the southern margin of the 
belt, the area south of Makataysip Lake contains significant base and precious metal vegetation geochemical 
signatures. A group of elevated percentiles for precious metals includes Au (98th – 30 ppb, 95th – 20 ppb), As (95th – 2 
responses, 3.4 ppm), Sb (99th – 1 ppm), Ag (100th – 1.4 ppm) and Br (100th – 110 ppm). The base metal assemblage is 
represented by Cu (99th – 286 ppm, 98th – 284 ppm), Pb (99th – 30 ppm), Ni (99th – 120 ppm, 98th – 104 ppm) and Fe 
(98th – 0.50%, 95th – 0.45%). Associated responses include K (100th – 20.44%), Hf (100th – 1.2 ppm), and 98th 
percentiles for Mn (30798 ppm), Ba (2100 ppm and two 95th percentiles, 1800 ppm), Mg (two 98th – 7.4% and three 
95th – 7.14%), Rb (780 ppm) and a 95th percentile for Cr (12 ppm). A cluster of elevated Cs responses are localized 
along the southern margin of the belt, as well as at the sedimentary-volcanic rock contact. These include the 100th (37 
ppm), 99th (25 ppm) and 98th (3 responses – 22 ppm) percentiles.

Similarly elevated precious and base metal responses were isolated in the east Sharpe Lake and west-central Sharpe 
Lake areas. The precious metal signatures of Au (98th – 30 ppb) and As (100th – 5.7 ppm, 98th – 3.8 ppm) and the base 
metal responses of Pb (98th – 26 ppm), Cd (99th – 3.4 ppm), Fe (99th – 0.46%) and an east-west linear trend of 99th 
(100 ppm), 98th (93 ppm) and 95th (82 ppm) percentiles for Ni are generally associated with long strike length airborne 
EM conductors. Associated responses include elevated percentiles for Ba (98th – 2 responses, 1800 ppm), Cr (98th – 
14 ppm), Mn (98th – 2 responses 30798 ppm), Mg (100th – 8.11%), V (98th – 10 ppm) and P (98th – 2 responses, 18462 
ppm). In the same manner that Rb and Cs defined significant regional differences in concentrations between the west 
end of the Edmund Lake belt (Margaret Lake area), and the east end of the belt in Manitoba (Little Stull Lake area), 
significantly elevated P concentrations are documented from the west end of the Sharpe Lake belt; in contrast P 
contents and very low east of Sharpe Lake.

The association of elevated vegetation geochemical responses with airborne EM conductors observed at Sharpe Lake 
is maintained in the west-central portion of the belt and is best illustrated by the results from the area south of Webber 
Lake. The area is characterized by elevated percentiles for Zn (100th – 4700 ppm), Cu (100th – 352 ppm, 98th – 284 
ppm), Pb (100th – 36 ppm), Fe (100th – 0.68%), REE (100th – 28.9 ppm, 98th – 17.7 ppm), Mg (100th – 8.11%), Cr (99th 
– 2 responses, 12 ppm), V (100th – 12 ppm), Mn (100th – 34296 ppm), Na (100th – 2900 ppm), Sc (100th – 2.1 ppm), Sr 
(98th – 898 ppm) and Rb (99th – 850 ppm, 98th – 780 ppm). Additional responses in this part of the belt include Ba (98th 
– 2 responses), Ag (100th – 1.4 ppm), K (99th – 28.9%, 98th – 28.35%), Cd (100th – 3.8 ppm, 99th – 3.4 ppm, 98th – 3 
ppm), P (100th – 19284 ppm, 98th – 3 responses, 18462 ppm) and Ba (100th - 478 ppm). Linear east-west trending 
anomalies are defined in the area west of Sharpe Lake to south of Webber Lake for Co (99th – 2 responses, 13 ppm, 
98th – 2 responses, 11 ppm, 95th – 9 ppm) and Cr (98th – 3 responses, 14 ppm, 95th – 12 ppm). Bleached, yellow 
stained, fractured, pyritic felsic intrusions near the west end of Sharpe Lake (sites 249 and 266) are marked by the 
100th percentile responses for Au (214 ppb), Mo (100th – 20 ppm), Ba (100th – 478 ppm) and Sb (99th – 1 ppm).

The small area of greenstone mapped north of the west end of Sharpe Lake and centered on Barclay Lake is 
characterized by an areally restricted, circular aeromagnetic response on its west shore. Vegetation geochemical 
responses from this area are marked by elevated percentiles of Fe (98th – 2 responses, 0.50%), Cr (100th – 21 ppm), 
Co (100th – 15 ppm, 98th – 11 ppm), Ni (100th – 128 ppm) and P (100th – 19284 ppm). These responses are suggestive 
of high-Mg source rocks; a carbonate-altered and epidotized mafic intrusion (diorite/gabbro) was documented from 
limited exposure on the west shore of Barclay Lake. Additional responses in the area include a base metal signature 
Zn (98th – 3200 ppm) and Pb (98th – 26 ppm), a 98th percentile response for Au (30 ppb), a 98th and 95th percentile for 
REE (17.8 and 16 ppm, respectively), a 98th percentile for K (18%) and three 98th percentiles for Ba (442 ppm).

Synthesis

The proliferation of multi-element, multi-sample high contrast vegetation geochemical signatures, defined in both 
greenstone belts surveyed in 1997, is somewhat surprising given the abundance of peat lands and other areas of 
significant and hostile clay-rich surficial deposits. This point is given further relevance by the fact that 80% of all b-
horizon soil samples collected in 1997 were developed in lacustrine clays deposited in glacial Lake Agassiz. Clearly, 
the nature of the surficial deposits in the study area has not proven to be a significant barrier to element migration and 
subsequent acquisition by the relatively shallow root systems of the black spruce (Picea mariana) trees. Moreover, the 
coincidence between areas of anomalous geochemical response for bedrock and vegetation samples indicates the 
vegetation anomalies are reflecting bedrock sources of metal concentrations associated with mineralization and 
related alteration zones, unique geophysical signatures and lithologies.

It is of considerable interest that the elements reflecting bedrock geological features of interest to mineral 
explorationists are defined on regional and more localized scales by both essential and non-essential elements. 
Examples of this are provided by both the Edmund Lake and Sharpe Lake greenstone belts. The area of the Margaret 
Lake intrusion and in general the west end of the Edmund Lake belt is marked by highly elevated Rb and Cs 
responses whereas the east end of the belt has very low contents of these elements. Rb is an element essential for 
plant metabolism whereas Cs is a non-essential element. A regional P enrichment west of the east end of Sharpe 
Lake in the Sharpe Lake belt and the low contents of this element in vegetation samples collected between Sharpe 
Lake and the Manitoba-Ontario border is based upon the geochemical flux of an element essential for energy 
metabolism in vegetation. Regional stratigraphic-structural features such as the contact between (i) Oxford Lake 
Group sedimentary and volcanic rocks (ii) Oxford Lake Group sedimentary rocks and Hayes River basalt, and (iii) belt 
margins are well defined by vegetation geochemical responses which include “ore and ore-related” elements (Au, As, 
Sb, Cu, Pb, Zn), elements indicative of unique lithologies (Ni, Co, Cr, Fe, P) and by essential elements such as K 
(plant metabolism). The entire contact of the Oxford Lake Group sedimentary rocks with associated basalts can be 
traced in its entirety by the K response in crown twigs. This is particularly relevant because it is this contact and 
associated faults that localize gold mineralization at the Twin Lakes and Seeber River deposits.

Localized, point-specific vegetation anomalies that correlate to bedrock sources are recognized throughout both 
greenstone belts with examples from the Wolf Bay Shear Zone (WBSZ) in the Edmund Lake belt, including the Little 
Stull Lake gold deposits and a gold occurrence in the Ken Bay area of Little Stull Lake, and the Twin Lakes and 
Seeber River gold deposits in the Sharpe Lake belt. An interesting mineral occurrence characterized by bleached, 
yellow-stained, fractured felsic intrusive rocks with up to 20% disseminated and veinlet pyrite mineralization was 
observed in an intensely burned area of the north shore of west central Sharpe Lake. Crown twig samples from this 
area are anomalous in Au, Mo, Ba and Sb and correspond to anomalies in these elements as well as U and Th in 
other sample media. Platinum group elements should be determined on rock chip samples of this site.

Conclusions

This vegetation geochemical survey based on the INA and ICP-AES analysis of ashed samples of the crown twigs of 
the black spruce (Picea mariana) tree indicates:

1)	geochemical flux in the ashed vegetation datasets define metallogenetically significant regional features as well as 
more localized bedrock point source mineralized zones, unique lithologies and anomalous magnetic and 
electromagnetic responses;

2)	the vegetation geochemical responses are based upon the variation in concentration of essential and/or non-
essential elements;

3)	the coincidence of vegetation geochemical anomalies with those defined by the analysis of outcrop rock chip, b-
horizon soil and humus samples suggests the relatively hostile, clay-rich surficial deposits are not necessarily 
“geochemically impenetrable” by the shallow root system of the black spruce tree;

4)	the observation of coincident vegetation and outcrop rock chip geochemical anomalies is also indicative of the lack 
of relevance of the observed range in ash content (1.7 – 2.7%) of crown twigs as pertains to the recognition of 
mineralized sites;

5)	new areas of interest, partially afforded by an intense forest fire along parts of the north shore of Sharpe Lake, 
have been identified by the survey and include altered and mineralized felsic intrusions at west Sharpe Lake (U-
REE-Au), the Oxford Lake Group sedimentary contact (Au-Ag), central and west shores of Edmund Lake (Au, Ni), 
the periphery of the Margaret Lake granite intrusion (base and precious metals), site of the WBSZ deflection (Au), 
Ken Bay area of Little Stull Lake (Au), and an area midway between Kistigan Lake and Margaret Lake (Au, Ni). 
The Barclay Lake outlier should be reconnoitered to assess the high-Mg, base and precious metal vegetation 
geochemical anomalies.



SYNOPSIS

The 1997 multimedia geochemical survey of the Edmund Lake and Sharpe Lake greenstone belts has successfully 
delineated geochemical patterns attributable to regional metallogenetic features (Wolf Bay Shear Zone, Margaret Lake 
granite intrusion and the Oxford Lake Group – volcanic and sedimentary subgroup contacts), as well as more localized 
signatures of known gold deposits in both belts. Additionally, high contrast multi-sample geochemical anomalies have 
been documented in areas of no known mineralization (south and west of Makataysip Lake, Sharpe Lake belt). Unique 
lithologies, such as high-Mg basalts and/or ultramafic rocks, have also been detected in this survey.

On The basis of the geochemistry of all sampling media, the area west of the east end of Sharpe Lake has 
geochemical characteristics suggestive of a base metal depositional environment, whereas the area east of Sharpe 
Lake would appear to be highly prospective for precious metals. The apparent association of multi-media geochemical 
signatures with the periphery of the mineralized Margaret Lake granite intrusion, as well as the association of an 
altered and mineralized quartz-feldspar porphyry at Little Stull Lake with five gold zones indicates the mineral potential 
for these areas.

The relatively high success rate between the various sample types in reproducing the geographic locations of 
geochemical anomalies is surprising given the extensive wetlands and peats in the 1997 survey area. With the 
exception of humus results in the area of the Twin Lakes – Seeber River gold deposits, all sample media identified the 
presence of known gold mineralization. Areas of anomalous geochemical response without known mineralization are 
also multi-media in nature. The general hostile nature of the surficial deposits in the 1997 survey area is reflected by 
the fact that 80% of b-horizon soil samples are lacustrine clay. Historically/traditionally this material has been viewed 
as having little value in mineral exploration, and has been considered to be very effective in concealing the 
geochemical response of buried or blind mineralized zones. The application of the enzyme leach process to these 
sediments has demonstrated that geochemical data useful in mineral exploration can be derived from this new 
approach. The success of the b-horizon/enzyme leach soil survey is mirrored by the equally successful vegetation 
geochemical survey, based on the collection of black spruce crown twigs. The shallow root system of this tree is often 
cited as problematic, limiting acquisition of metals to those derived from often allochthonous near surface deposits. 
The trees sampled in 1997 were observed to be rooted in the same glaciolacustrine clays as were sampled for 
enzyme leach analysis and suggests the essential and non-essential elements required for proper nutrition are being 
derived, in part, from this soil horizon. It would appear that the process or mechanism of metal dispersion from bedrock 
sources (groundwater and/or vapour phase transport?) may be slowed by “hostile” surficial deposits but it is not 
prevented.

Although carbonate abundance in the glacial tills sampled for analysis has not yet been determined, the tills are highly 
calcareous and as such would appear to have diminished effectiveness in geochemical prospecting. Element mobility 
in carbonate/alkaline environments is significantly reduced. Nevertheless, multiple high contrast geochemical 
responses in the <2µm and <63 µm size fractions of till were documented from both greenstone belts. The reason for 
this is uncertain and in an attempt to provide an explanation carbonate contents are being determined by the 
Geological Survey of Canada for both 1996 and 1997 till samples. Regardless of carbonate content, glacial till has 
proven to be an effective geochemical prospecting tool for this area.

The ability to land a helicopter at approximate 1 km sample spacings in areas of intense burn provides an excellent 
opportunity to examine outcrop areas previously covered or obscured by vegetation and/or sediment. The potential for 
observing significant indications of hydrothermal alteration and mineralization was apparent in the 1996 survey, where 
areally extensive massive sulphide type alteration was identified at Max Lake. In the 1997 survey, two areas of 
potentially significant geological observations were made at sites 249 and 266 in the Sharpe Lake belt and at sites 80, 
82 and 83 in the Edmund Lake belt. At sites 249 and 266 fractured, bleached, bright yellow-stained fine to coarse 
grained felsic intrusions with up to 20% disseminated and veinlet pyrite are exposed. The sample media from this 
occurrence are characterized by a REE-U-Sb metal assemblage (63 and 10 ppm Sb in rock). Platinum group element 
analyses should be undertaken on rock chip samples from these occurrences and the area between the two sites and 
beyond should be thoroughly prospected to determine the nature of this occurrence. Base metal, massive sulphide 
type alteration is exposed at sites 82 and 83 where diffuse to wispy iron oxide veinlets are observed in pillow selvages 
and pillow basalts in association with intense silicification and an outcrop of intrusive breccia. The zone is exposed for 
several tens of metres at the shoreline of a small lake and appears to be continuous along strike. Site 80 is marked by 
two pieces of float that are angular, highly silicified, cherty rocks with pyrite laminae. The samples were collected from 
the shore of a small linear lake and are interpreted to be short transport erratics because of their general fragile nature. 
This float could have been brought to surface by permafrost/frost jacking and is representative of a strongly 
hydrothermally altered lithology. Areas of recent (1988-89) burn should become priorities for geological examinations.

The most significant area of multimedia geochemical anomalies occurs south and west of Makataysip Lake. The 
contact between Hayes River basalt and Oxford Lake Group sedimentary subgroup rocks is present in this area and 
represents a prime metallogenetic feature. The Twin Lakes and Seeber River gold deposits are localized at or near 
this contact, which represents an exciting regional geological feature with excellent residual exploration potential. The 
highest As contents measured in any sample media occurred in a humus sample from the area south of Makataysip 
Lake and includes a 1300 ppm and a 38 ppm As analysis.

The small greenstone – intrusive outlier at Barclay Lake in the Sharpe Lake belt should be reconnoitered based on its 
circular aeromagnetic response and multiple moderate to high contrast geochemical anomalies.

The significant of the rapid and cheap measurement of H+ (pH) and specific conductance (conductivity) in rock and soil 
samples has been demonstrated in the 1997 survey results. Water-extractable metal (specific conductance) 
measurements are generally associated with high metal contents in rocks and soils and can provide an effective pre-
screening tool in surveys of this type.

KIMBERLITE INDICATOR MINERAL SURVEY

Introduction

Mineral such as garnet, chromite, ilmenite and diopside have been used as indicators of kimberlite. Specifically the 
chemistry of these grains has been used to imply their mode of occurrence in diamonds as inclusions or in kimberlites 
(cf. Dawson and Stephens, 1975; Gurney, 1984 and McCallum and Vos, 1993).

Garnets have received considerable attention as kimberlite indicators and have been chemically classified according 
to their relevance as kimberlite indicator minerals (KIM). Garnets that are Ca-depleted diamond inclusion chrome 
pyropes have been termed “GIO” (Gurney, 1984; Dawson and Stephens, 1975). Dawson and Stephens (1975) 
indicate that the recognition of GIO garnets in overburden is very important. These garnets indicate a harzburgitic 
peridotite origin and are more closely associated with diamonds than are the garnets of lherzolitic origin, which are 
termed “G9”. Eclogitic garnets, with Na20 concentration of greater than 0.09%, have been observed as inclusions in 
diamonds and as such represent valuable kimberlite indicator minerals.

Diamond inclusion chromites with Cr203 of greater than 60% are considered to be kimberlite indicator minerals, equal 
in significance to GIO garnets. Chrome diopside with greater than 1% Cr203 has been utilized as a useful kimberlite 
indicator mineral (Morris et al., 1994). Kimberlite-hosted ilmenite generally has Mg0 concentrations of 4-15 weight % 
and greater than 2% Cr203.

Sample Collection

An eleven litre pail of glacial till was collected from each sampling site where appropriate material was encountered. 
These samples were shipped to MONOPROS Ltd. at the end of the 1997 sampling program for processing. A total of 
186 samples were collected with 149 coming from the Edmund Lake belt and 137 from the Sharpe Lake belt.

Sample Preparation and Analysis

The eleven litre samples were screened at 2.0 mm, with the oversize discarded except for a representative aliquot of 
the +2.0 – 5.6 mm fraction, which is used for pebble counts. The –2.0 mm size fraction was passed over a 0.3 mm 
aperture sieve and the –0.3 mm size fraction was discarded. The +0.3 mm – 2.0 mm fraction was concentrated by 
gravity separation, dried in ovens and the further sieved into +1.0-2.0 mm, +0.5-1.0 mm and +0.3-0.5 mm size 
fractions, which were packaged, labelled and shipped to MONOPROS laboratories for further treatment.

These three size fractions were individually separated using the heavy liquid bromoform (Specific Gravity – 2.86). The 
heavy fractions that sink through the bromoform were washed and sorted for kimberlitic indicator minerals. Indicator 
minerals were analysed by microprobe. This paraphrased description of sample preparation and analysis was supplied 
by MONOPROS Ltd.

Data Display

Abundances of kimberlite indicator minerals are portrayed using bubble plots. The greater the abundances of any 
particular indicator mineral at a sample site the larger the bubble.

A mylar sample site location map overlay is available for purposes of overlaying the bubble plots.


PRELIMINARY INTERPRETATION OF THE 1997 KIMBERLITE INDICATOR MINERALS SURVEY

The chemistry of KIM picked and microprobed for this study are summarized in Appendix 1 and their abundances by 
sample site is given Appendix 11. Classification, based on mircoprobe chemistry in Appendix 1, utilized the chemical 
parameters in Tables 3 and 4 taken from Thorleifson et al., (1994). A sample site location map for both the Edmund 
Lake and Sharpe Lake greenstone belts is provided in Figure 3a. Figure 3b is a mylar sample site location map 
overlay. Kimberlite indicator mineral abundances from each belt are presented in Table 5.

	Results of 1997 Overburden Sampling

Figure 5 through 10 are bubble plots for individual kimberlite indicator minerals (KIM) throughout the 1997 survey area. 
These plots represent KIM from combined +1.0-2.0 mm, +0.5-1.0 mm and +0.3-0.5 mm size fractions of the sample. 
Total KIM abundances are plotted in Figure 11. It is important to note that bubble plots for KIM data portray all sites at 
which a sample was collected. To gain a true appreciation for the significance of these geographic distributions and 
clustering, these maps should be viewed using the mylar overlay depicting all multimedia sample locations. Survey 
results for each of the Edmund Lake and Sharpe Lake greenstone belts are described below and summarized in Table 
3.

	Edmund Lake Belt

A total of 43 KIM grains were retrieved from the 149 samples collected within the mapped limits of this belt. There were 
not G10 or Ti-Cr pyrope garnets identified in the Edmund Lake samples and the diffuse geographic distribution of 
chrome spinel and chrome diopside grains (Figs. 5, 6) is interpreted to be non-definitive.

The distribution of G9 garnets is somewhat different, with a four sample cluster identified in the immediate area of the 
Little Stull Lake gold deposits and a second three sample cluster near a small lake midway between Margaret Lake 
and Little Stull Lake on the Wolf Bay Shear Zone (“WBSZ”, Fig. 8). A seven sample cluster of Mg-ilmenite grains is 
also developed in the area of the three sample G9 cluster (Fig. 10). A four grain Mg-ilmenite cluster occurs southeast 
of Margaret Lake.

The plot of total abundances in the Edmund Lake belt (Fig. 11) enhances the Mg-ilmenite-dominated KIM signature at 
the mid-point of the WBSZ. Interestingly, this general area is the site of multi-media geochemical anomalies for Ni, Mg, 
Ti and Cr in rock samples as well as Ti in both till and b-horizon soil samples and is suggestive of a high-Mg source 
lithology. The site is worthy of ground follow-up.


Table 3.  Guidelines for preliminary mineral identification (Thorleifson et al., 1994).

Total <70%	+ CA0 >44%	Apatite
Total <70%	+ Fe0 >50%	Siderite
Total <70%	+ Al203 >40%	Gahnite
Total  34%	+ Si02  33%	Zircon
Total <70%			low total; e.g. phosphate sulphate, 
carbonate

Si02 <20%	+ Cr203 >60% + Mg0 >12%	diamond inclusion Cr-spinel
	+ Cr203 >10%	Cr-spinel
	+ Ti02 >70%	Rutile
	+ Ti02 >30% + Mg0 >6%	Mg-ilmenite
	+ Ti02 >30%	Ilmenite
	+ Ti02 >1%	Ti-Fe-oxide
	+ Fe0t >90%	Magnetite
	+ Fe0t >80%	Hematite
	+ Fe0t >40%	Goethite
	+ Al203 >80	Corundum
	+ Al203 >30% + Fe0 >20%	Hercynite
	+ Al203 >30%	Spinel

Si02 >75%			Quartz
Si02 >55%	+ Al203 >16%	Feldspar

Ti02 >20%			Sphene

Al203 >55%			Kyanite
Al203 >45%			Staurolite
Al203 >24%	+ total <90% + Mg0 >5.3%	Mg-tourmaline
Al203 24%	+ total <90% + Mg0 <5.3%	Fe-tourmaline
Al203 24%	+ total<98% + Ca0 22.2-25%	Epidote

Si02 <47%	+ K20 >0.5% or Na20 >1%	
	or Si02 41-47% _ Cr203 <0.5%	Amphibole

Si02 >47%	+ Ca0 <3.1%	OPX
	+ Na20 >2.7%	Na-CPX
	+ Fe0t >6.1%	Fe-CPX
	+ >0.5% Cr203	Cr-diopside
	Remainder	Diopside

Mg0 >25%			Olivine

Garnet	+ Mg0 >13% + Cr203 >0.5%	Cr-pyrope
	+ Mg0 >4% + Ca0 >2% + Ti02 >0.2%	Eclogitic garnet
	+ Cr203 >14%	Uvarovite
	+ Mg0 >13%	Pyrope
	+ Ti02 >2.5 + Al203 <11.5%	Melanite
	+ Ca0 >16% + Al203 <11.5% + Cr203 >1%	Cr-andradite
	+ Ca0 >16% + Al203 <11.5%	Andradite
	Ca0 >30% + Cr203 >1%	Cr-Grossularite
	+ Ca0 >30%	Grossularite
	+ Mn0 >21%	Spessartite
	+ Fe0t >25%	Almandite
	Remainder	Garnet

Table 4.  Kimberlite indicator mineral classification (Thorleifson et al., 1994)

1.	Cr-spinel	>60% Cr203 + >12% Mg0	diamond inclusion Cr-spinel

2.	Ilmenite	>-6% Mg0	Mg-ilmenite

3.	Pyroxene	>0.50% Cr203	Cr-diopside

4.	Garnet	>13% Mg0 and >0.50% Cr203	Cr-pyrope

		>0.30% Ti02 + 4.0% Cr203	G11 titanian, Cr-pyrope
		>90% Ti02	G2 titanian, Cr-pyrope
		>0.30% Ti02	G1 titanian, Cr-pyrope

		>12.0% Cr203	G12 Non-titanian, Cr-pyrope

		Ca0 <0.285 (Cr203)+3.14	G10 Non-titanian, Cr-pyrope
		Ca0 >0.285 (Cr203)+5.14	G7 Non-titanian, Cr-pyrope
		Remainder	G9

		>4.0% Mg0 + >2.0% Ca0 + >0.20% Ti02 +	Eclogitic garnet
		>19% Al203 + <0.5% Cr203

		>0.60% Ti02	G4
		>16.0% Ca0	G8
		>12.0% Ca0	G6
		Remainder	G3

	Site	Cr-Spinel	Chrome	Ti-Cr	G9	G10		Mg-
			Diopside	Pyrope			Ilmenite

1.	Edmund Lake Belt	5	7	nil	16	nil	5

2.	Sharpe Lake Belt	6	2	3	11	1	14





Table 5.  Summary of the geographic distribution of kimberlite indicator mineral grains.

	Sharpe Lake Belt

Thirty-seven KIM grains were identified in 137 samples from the belt. The distribution of chrome spinel (Fig. 5), chrome 
diopside (Fig. 6), titanian-chrome pyrope garnets (Fig. 7) and G9 garnets (Fig. 8) are interpreted as non-definitive. A 
single G10 garnet was identified in a sample collected from the eastern end of Sharpe Lake (Fig. 9). The distribution of 
magnesian ilmenite (Fig. 10) in the belt is also diffuse except for a six grain cluster over a short stretch of the belt 
south and east of Webber Lake.

A small greenstone outlier just north of the west end of Sharpe Lake is marked by chrome spinel, a titanian-chrome 
pyrope garnet, and two grains of magnesian ilmenite. These minerals are probably related to a gabbroic intrusion 
identified in outcrop at Barclay Lake.

The plot of total abundances in Figure 11 reflects the generally scattered nature of the KIM grains in this belt. The area 
of the G10 garnet should be reconnoitered, although its occurrence as a single grain may suggest it has been derived 
from a distal source.



