The DOD showing occurs within the Slave Supracrustal Province,
Archean in age.  The Supracrustal rocks are of the Yellowknife
Supergroup, dominated by a volcanic-greywacke-mudstone sequence
forming various greenstone belts that cover about one third of the
province.  Granitoid intrusions make up the bulk of the craton and
are grouped as pre-, syn-, and post- Yellowknife Supergroup.  In
addition, several mafic dykes have intruded the shield, orientated
between 140 and 180 degrees.    The DOD showing is situated on the
Camsell Lake property which is approximately 20 miles north of the
East Arm of Great Slave Lake.  The rocks on the Camsell property
are volcanics and sediments of the Yellowknife Supergroup which
occur as two northeasterly trending belts. These belts have been
intruded by glomeroporphyritic leucogabbro/gabbro stocks, gabbro
sills and rare leucogabbro sills.  Granitic intrusions include
dykes and stocks of granodiorites of various compositions and
pegmatites of the same phases.  All rocks of the area are intruded
by north-northwesterly magnetic diabase dykes.  This showing is a
Cu-Ni mineral occurrence from two drill holes. The mineralization
is disseminated in a gabbroic volcanic and ranges from 0.23% Cu
over 10 feet to 0.45% Cu over 2.2 feet and 0.11% Ni over 10 feet to
0.12% Ni over 5 feet.  The showing was discovered after geophysical
work in 1967 located an anomaly.  The anomaly was then drilled and
trenched, although no report can be located with the information.
No further work on the area has since been reported.
This showing was derived from the CANMINDEX database.  No mention
of this showing is located in any assessment report and is only a
mineral occurrence on a map.  In the GSC paper 70-70, the EGO claim
group is mentioned to be owned by Shield Resources in 1966.
The CL 25 showing occurs within the Slave Supracrustal Province,
between 140 and 180 degrees.  Also present in the regional area are
diamondiferous kimberlite pipes that occur along the same general
strike as the dyke swarms.  The CL 25 showing is situated on the
by north-northwesterly magnetic diabase dykes.  Although past
mineral exploration was focused on the Cu-Zn potential on the
Camsell Lake area, diamond exploration has been the main focus
since the first discovery of kimberlites in the Slave.  Winspear
Resources Inc., Aber Resources, Amarado and Consolidated Newgate
started work on the Camsell Lake project in 1993 with a regional
airborne Mag/EM survey was completed.  Following the survey,
samples were collected from two major eskers in the southern
portion of the property.  In 1994, a ground survey and basal till
sampling and diamond drilling was completed.
Results from the 1994 field season included plotting indicator
minerals on maps from sample locations to trace back towards the
possible source.  By combining information from geophysical surveys
and sampling results, four drill holes tested two geophysical
anomalies.  Three drill holes intersected kimberlites.  From drill
holes 1 and 2 a bulk sample weighing 350.4 kg contained a total of
221 diamonds; 9 were macro- (>0.5 mm) and 212 micro-sized (<0.5 mm).
These intersections of kimberlite resulted in the discovery of
the first kimberlite pipe on the Camsell Lake Property.
The CL 174 showing occurs within the Slave Supracrustal Province,
strike as the dyke swarms.  The CL 174 showing is situated on the
The CL 174 kimberlite pipe is 150 metres northwest of the CL 25
kimberlite pipe.  Its discovery came when drilling to find the
extent of the CL 25 pipe was done.  The only information on the
showing to date is that from news releases stating from drill hole
174-1 a 622.2 kg sample was taken and 284 total diamonds were
recovered, with 274 micro- (<0.5 mm) and 10 macro-sized (>0.5 mm).
The CL 186 showing occurs within the Slave Supracrustal Province,
strike as the dyke swarms.  The CL 186 showing is situated on the
Resources started work on the Camsell Lake project in 1993 with a
regional airborne Mag/EM survey was completed.
The CL 186 showing is a diamondiferous kimberlite pipe on the east
shore of Snap Lake.  Despite the presence of kimberlite boulders,
the area gives a low magnetic response due to 100 metre of granite
overlying (and masking) the kimberlite pipe.   After drilling into
kimberlite breccia in 1997, diamond analysis of two bulk samples
resulted in a total of 11 diamonds from a 74.2 kg sample and 114
diamonds from a 78.2 kg sample.  The two samples produced a total
of 42 macro-sized diamonds.
The Snap Lake Dyke showing occurs within the Slave Supracrustal
Province, Archean in age.  The Supracrustal rocks are of the
Yellowknife Supergroup, dominated by a volcanic-greywacke-mudstone
sequence forming various greenstone belts that cover about one
third of the province.  Granitoid intrusions make up the bulk of
the craton and are grouped as pre-, syn-, and post- Yellowknife
Supergroup.  In addition, several mafic dykes have intruded the
shield, orientated  between 140 and 180 degrees.  Also present in
the regional area are diamondiferous kimberlite pipes that occur
along the same general strike as the dyke swarms.  The Snap Lake
Dyke showing is situated on the Camsell Lake property which is
approximately 20 miles north of the East Arm of Great Slave Lake.
The rocks on the Camsell property are volcanics and sediments of
the Yellowknife Supergroup which occur as two northeasterly
trending belts. These belts have been intruded by
glomeroporphyritic leucogabbro/gabbro stocks, gabbro sills and rare
leucogabbro sills.  Granitic intrusions include dykes and stocks of
granodiorites of various compositions and pegmatites of the same
phases.  All rocks of the area are intruded by north-northwesterly
magnetic diabase dykes.  Although past mineral exploration was
focused on the Cu-Zn potential on the Camsell Lake area, diamond
exploration has been the main focus since the first discovery of
kimberlites in the Slave.  Winspear Resources Inc., Aber Resources,
Amarado and Consolidated Newgate Resources started work on the
Camsell Lake project in 1993 with a regional airborne Mag/EM survey
was completed.
The Snap Lake Dyke has been intersected 11 times in an area of 1
square km.  The dyke, with an average true thickness of 2.47 metres,
was bulk sampled  with a total of 137.14 kg of kimberlite
recovering 401 diamonds, 149 macro- (>0.50 mm) and 252 micro-sized
(<0.5 mm).
The Snap Lake Boulder showing occurs within the Slave Supracrustal
Boulder showing is situated on the Camsell Lake property which is
The Snap Lake Boulder showing is 6 boulder samples taken on the
northwest shore of Snap Lake that had diamonds in them.  The total
weight of the samples taken was 248.18 kg in which 637 diamonds
were found, 202 macro- (>0.50 mm) and 435 micro-sized (<0.5 mm).
Regional: The TALL claims are located on the western side of the
Courageous Lake Archean Greenstone belt which is a 60 km long north
south striking volcanic belt within the Yellowknife Supergroup.
Property: The TALL property is composed of volcanics which are
overlain to the east by Yellowknife Supergroup sediments and
undermined to the west by granites.  Showing: Noranda drilled six
airborne electromagnetic conductors in 1980 some of which
represented massive sulphide zones in felsic tuffs.  One of the
holes, T-4-80, tested a 300 - 400 metre EM conductor with
coincident mag which contained a 1.02 metre zone at a felsic
pyroclastic-mafic tuff contact.  This zone contained massive
pyrrhotite and pyrite as well as traces of chalcopyrite and 0.67%
zinc in sphalerite.  No further work was recommended.
Regional: The CAM property lies in the central, volcanic portion of
the Camsell Lake Greenstone Belt of Archean aged Yellowknife
Supergroup volcanic and sedimentary rocks of the Slave Province.
Property: volcanic rocks in the area are composed of locally
pillowed basalts and andesites with some felsic tuff beds.  These
units are intruded by a well-differentiated gabbro-anorthosite
complex which also strikes NE-SW.  The volcanic rocks are cut by
fairly prominant shears which run both parallel and at acute angles
to the volcanics.  The entire package is underlain by Proterozoic
granites.  Showing:  The property was originally staked in 1957 as
the LIZ group and optioned to Cominco who did geophysics, trenching
and drilling in 1958, finding fair copper values.  The property was
then re-staked in 1964 as the CAM group and more geophysical work
was done.  In 1966 the property was optioned by Hurley River Mines
who did more geophysics and 2,607 ft. of drilling which resulted in
up to 5.2 feet grading 0.47% Cu and minor zinc.    In general the
mineralization consists of fairly massive po. with minor associated
cpy, and traces of sph.  Two major types of mineralization have
been observed, both occuring in shear zones in the altered
volcanics, near and parallelling the volcanic-gabbro contact. Type
1 - Cpy-po-py bearing altered andesite and associated massive
mineralized quartz. Type 2 - Fine grained po-mt-py disseminated
along shear zones in the altered andesite. The cpy type of
mineralizaion occurs at several localities on the property.
Regional: The PEP property lies in the central, volcanic portion of
pillowed basalts, andesites and dacites with some felsic tuff beds.
These units are intruded by a well-differentiated gabbro-
anorthosite complex which also strikes NE-SW.  The volcanic rocks
are cut by fairly prominant shears which run both parallel and at
acute angles to the volcanics.  The entire package is underlain by
Proterozoic granites.  Showing:  The author could not find the
early work done on this showing though the property was first
prospected in the mid 1960s.  The only other work done on the claim
was in 1971 when Anglo United Development ran a ground geophysical
survey  over the prospect and drilled three diamond drill holes
through the shear to test a coincident anomaly at depth. In general
the mineralization occurs in a shear near to and parallelling the
volcanic-gabbro contact and consists of fairly massive po. with
minor associated py and  cpy. The results were poor with copper
values up to 0.27%, and zinc up to 0.22%.
During 1948, 345 feet of diamond drilling was recorded on the
SECUM11 claim by J. McAvoy for  Cunaxa Mining Ltd.  This property
is located in the Courageous Lake area of the Yellowknife
Supergroup in a peninsula in McKay Lake.  Some pyrite, pyrrhotite,
chalcopyrite and trace  galena mineralization was reported, however
no further work has been recorded.  Drilling was  also completed on
the adjacent KM12 claim.
During 1948, 500 feet of diamond drilling was recorded on the KM 12
claim by J. McAvoy for  Cunaxa Mining Ltd.  This property is
located in the Courageous Lake area of the Yellowknife Supergroup
in a peninsula in McKay Lake.  Pyrite, pyrrhotite, chalcopyrite and
galena were reported, however no further work has been recorded.
Drilling was also completed on the adjacent SECUM 11 claim.
Known as the Roma and Jeta claims in 1945-1950, held by Homer YK
mines, no assessment report found.  Known as the Don claims in 1958,
held by North Goldcrest mines, no assessment report found, and in
1973 (also Don claims) held by Golden Ram resources, no report
found.
Regional: The Courageous-MacKay Lake Greenstone Belt is one of the
twenty volcanic belts within the  Slave Structural Province which
make up the volcanic portion of the Yellowknife Supergroup. The
greenstone belt is an eastward facing, homoclinal sequence of
volcanic rocks overlain by a thick sedimentary group. The Matthews
Lake Volcanic Complex is composed of pyroclastic and volcanoclastic
units of  rhyodacite to rhyolite composition.  Mafic flows and
interflow sediments make up a minor portion of this complex.  All
of the gold showings on the Tundra property are associated with the
volcanics of this complex.  Property: The Matthews Lake Volcanic
Complex  may be divided into two volcanic cycles characterezed by
mafic flows to felsic pyroclastic successions.  The top of  each
cycle contains localized gold mineralization within felsic ash and
lapilli tuff in assiciation with blue quartz veins and arsenopyrite
mineralization.  Showing: The main BERTHA 5 showing is descibed as
felsic lapilli tuff with 1% py., and 1% aspy., foliated at 342
degrees and dipping 85 degrees to the west.  The surounding geochem
samples are described as having  up to 15% blue black quartz
veining and up to 10 % banded aspy.  Chlorite rich bands are also
noted in the logs. A second, satelite showing 150 m to the NW is
descrbed as wacke, near a mafic tuff contact with simmilar
minerology to the main showing.
Regional: The Courageous-MacKay Lake greenstone belt is one of the
twenty volcanic belts within the Archean Slave Structural Province
which make up the volcanic portion of the Yellowknife Supergroup.
The greenstone belt is an eastward facing, homoclinal sequence of
volcanic rocks overlain by a thick sedimentary group.  The Matthews
units of rhyodacite to rhyolite composition.  Mafic flows and
Complex  may be divided into two volcanic cycles characterized by
lapilli tuff in association with blue quartz veins and arsenopyrite
mineralization.  Showing: Assessment report 082777 describes three
samples which graded over 500 ppb gold.  These are of felsic and
intermediate ash tuff beds with up to 20% quartz veining and up to
3% aspy., 3% py., trace cpy., and 5 % epidote.  The showings all
had foliation striking from 338 to 004 degrees and dipping steeply
eastwards.
mineralization.  Showing: Assessment report 082777 describes one
sample gradomg 1040 ppb gold.  This is of a felsic lapilli tuff bed
with quartz veining and up to 1% py. The zone is 1 m wide.
mineralization.  Showing: The HARE 8 showing is a single chip
sample taken from an in situ frost heave by Noranda in 1988
(assessment report #82777). The sample was of a felsic ash tuff
with 75% aphanitic quartz, 10% sericite, 5% biotite, 5% chlorite,
2% py, and 1% po.  The sample graded 1150 ppb.
Regional: The Susu Lake Cu showing is situated within the Indian
Mountain greenstone belt which comprises mainly Archean Yellowknife
Supergroup supracrustal rocks. The belt is as much as 15 miles wide
and extends 40 miles north from Great Slave Lake.  The belt is
bounded on the east and west by granitic and migmatitic rocks but
has a core of relatively low grade metamorphic rocks(Heywood and
Davidson 1969).  The belt is seen to lie on deformed granitoid
rocks in some places and in others to be intruded by granitic
plutons of closely related age.  Property: The property in which
this showing occurs, lies approximately 8 miles west of Susu Lake.
It comprises a volcanic belt that is part of the larger Indian
Mountain greenstone belt.  The volcanic belt is dominated by
rhyolites with quartz-biotite-cordierite schists.  Deformation in
the area includes shearing and brecciation.  Intrusions of quartz
veins are also noted.  Showing: The Susu Lake Cu showing occurs in
a brecciated shear zone that hosts disseminated chalcopyrite and
bornite.  Mineralization is largely hosted by rhyolites, but also
occurs in neighboring quartz-biotite-cordierite schists.  Reserves
were calculated at 142,500 tons grading 0.95% Cu in 1967 from 9
diamond drill holes that were drilled by Indian Mountain Metal
Mines.  No other work on the showing has been recorded to date
although in Canadian Mineral Deposits Not Being Mined in 1989, it
was mentioned the property had been sold to Ego Resources.
The BB prospect is one of three related volcanogenic massive
sulphide occurrences situated in the Indian Mountain greenstone
belt in the southern Slave structural province. All stratified
rocks have been mapped as belonging to the Archean Yellowknife
Supergroup. The base of the stratigraphic sequence in the vicinity
of the deposits comprises a series of mafic tuffs with minor,
massive and pillowed mafic flows. The bottom of this unit is
migmatized. Overlying this mafic base are intermediate tuffs and
flows and then a felsic unit including massive rhyolite,
intermediate to felsic coarse pyroclastics, tuff, lapilli tuff and
tuff breccia. Sulphide deposits are hosted by a 1 - 10 metre thick
unit of carbonate-rich exhalite and pyritic cherty tuff, overlying
or near the top of the felsic unit. The stratigraphic succession is
completed by greywackes and argillites. All stratified rocks have
been metamorphosed to middle amphibolite facies.
The BB massive sulphide deposit consists of a series of closely
spaced lenses interbedded with and grading into highly altered
siliceous limestone which is probably a carbonate-rich exhalite.
Layers of coarse grained pyrite and sphalerite are interbedded with
layers of coarse grained pyrite and bands of massive, fine-grained
sphalerite. Galena occurs as small grains and blebs within massive
pyrite and sphalerite and as rims on host rock fragments in the
latter. Small blebs of chalcopyrite are scattered throughout the
deposit. Associated metallic minerals include minor amounts of
chalcopyrite, pyrrhotite, marcasite, magnetite and tetrahedrite.
Reserves were calculated for the BB showing and several values were
reported, increasing in tonnage as the number of drill holes
increased.  By the end of 1952, over 23,000 feet total drilling on
the property had been completed and reserves were calculated at 924,
000 tons grading 10.3% Zn, 0.85% Pb and 3.45 oz/ton Ag.    The BB
Lake Copper zone is situated within a discordant alteration pipe/
stringer zone underlying the BB and Kennedy Lake stratiform
mineralization. Chalcopyrite and pyrrhotite occur as stringers,
layers and seams in two bands 8 - 13 metres wide and up to 200
metres long. Sulphides in the higher grade portions of these bands
are accompanied by a black, unidentified amphibole. The alteration
pipe within which this stringer mineralization is located is zoned.
An inner, intensely altered zone consists of garnet, anthophyllite,
cummingtonite, cordierite, sericite and sillimanite in a less
intensely altered envelope which is characterized more by biotite,
quartz and chlorite.
Work on the BB showing began in 1948 when the property of which the
showing lies was discovered for McAvoy and was optioned off to
Hollinger Gold Mines.  Diamond drilling was started on the property
the following year.  Over 15,825 feet of core was drilled and
reserves were calculated at 270,000 tons of ore averaging 15.68% Zn,
1.67% Pb and 5.21 oz./ton Ag to a depth of 400 feet.  In 1951,
under the ownership of Indian Mountain Metal Mines Ltd., reserves
were re-calculated after drilling to the 800 foot horizon.
Information of the drilling program done in 1951, gave good enough
results for another 25,000 feet of drilling to be proposed for the
following year.  By the end of 1952, the BB zone had been drilled
to the extent of 23,000 feet and the amount of reserves for the
zone increased to 924,000 tons.  Plans were under consideration for
underground development and mill construction for 1953, but were
not implemented.  In 1965, extensive electromagnetic and
magnetometer surveys were done by Indian Mountain Metals Mines Ltd.
to re-examine the entire volcanic belt.  In 1966, drilling was done
on anomalies that were outlined the year before in the Kennedy Lake
area.  After 1966, no work on the BB zone has been reported.  The
property went to lease in 1974 and in 1979 the property was
optioned to Ego Resources. The Kennedy Lake Zone which lies under
Kennedy Lake is described in AR 061728 as the western extension of
the BB zone although it is separated from the latter by a barren
zone.  The zone is not exposed at the surface although drilling
outlined it to be 120 feet long with a maximum width of 21 feet.
The ore is similar in all respects to that of the BB zone.
Reserves for the Kennedy Lake zone were calculated at 43,000 tons
grading 7.3% Zn, 1.1% Pb and 4.0 oz./ton Ag.
The COTTONGRASS Au showing lies in the Archean Slave Structural
Province, in the Indian Mountain Greenstone belt.  It is hosted
within rhyolite rocks approximately 2 metres wide, that have been
metamorphosed to granulite facies.  The sample is defined by a
single grab sample that assayed 680 ppb of Au.
Regional The Dawn & Gem-1 showing is situated within the Indian
Mountain greenstone belt which is mainly Archean Supracrustal rocks.
Composed of volcanic and sedimentary rocks, it is as much as 15
miles wide and extends 40 miles north from Great Slave Lake.  The
belt is bound on the east and west by granitic and migmatitic rocks
but has a core of relatively low grade metamorphic rocks(Heywood
and Davidson 1969).  The belt is seen to lie on deformed granitoid
plutons of closely related age.  Property Rocks in the property
area are almost entirely of volcanic origin and consist of flows,
pyroclastics, and associated dykes and sills from felsic to mafic
in composition.  The rocks of the property have been folded,
striking approximately north-south, and are crosscut by a fault
that is directly north of the showing. Showing Mineralization is
within rhyolitic volcanic flows and occurs mainly as sphalerite,
galena and silver.  Its occurrence can be massive, disseminated or
as blebs within the host rock.  Some minor chalcopyrite, pyrite and
arsenopyrite are also associated with the mineralization.  Assay
results from 3 diamond drill holes with total length of 2159 feet,
range from 0.90% Pb over 2.5 feet to 0.97% Pb over 2.5 feet and 0.
41% Zn over 2 feet to 6.01% Zn over 1.5 feet.  The silver also had
assay results but no measurements are given and thus not reported.
Exploration Work in the area began after the discovery of the BB
zone in 1948, just south of the Dawn & Gem-1 showing.  The area was
staked in 1957 and 1958 by the McAvoy Option Group.  The property
was then optioned off to Mount Wright Iron Mines Company Ltd. in
1958 and in 1959 they drilled 39 holes in the showing vicinity.  An
EM survey was done on the showing in 1958.  In 1966, more
geophysical surveys were completed over the showing as well as 8
holes were drilled by Indian Mountain Metal Mines Ltd.  From this
drilling 3 holes intersected mineralization and the define the
showing.  No further work was completed on the area until 1992 when
Taiga Consultants Ltd. on behalf of Royal Oak Mines, Asamera
Minerals Inc. and Nebex Resources Ltd. did an EM survey over the
showing.
Regional The Dawn & Gem-2 showing is situated within the Indian
It is as much as 15 miles wide and extends 40 miles north from
Great Slave Lake.  The belt is bound on the east and west by
granitic and migmatitic rocks but has a core of relatively low
grade metamorphic rocks(Heywood and Davidson 1969).  The belt is
seen to lie on deformed granitoid rocks in some places and in
others to be intruded by granitic plutons of closely related age.
Property Rocks in the property area are almost entirely of volcanic
origin and consist of flows, pyroclastics, and associated dykes and
sills from felsic to mafic in composition.  The rocks of the
property have been folded, striking approximately north-south, and
are crosscut by a fault that is directly north of the showing.
Showing Mineralization is found within rhyolitic volcanic flows and
occurs mainly as chalcopyrite, sphalerite and silver.  Its
occurrence can be massive, disseminated or as blebs within the host
rock.  Some minor galena, pyrite and arsenopyrite are also
associated with the mineralization.  Diamond drilling from one hole,
AR 017123, ran assay results ranging from 0.2% Cu over 4 feet to 0.
88% Cu over 3 feet and 0.67% Zn over 5 feet to 1.66% Zn over 4 feet.
From AR 017122, 11 holes were drilled with a total of 1791 feet,
however only 8 holes intersected mineralization.  Assay results
from these holes ranged from 0.27% Cu over 48 inches to 3.98% Cu
over 24 inches. The silver also had assay results but no
measurements are given and thus not reported.
zone in 1948, just south of the Dawn & Gem-2 showing.  The area was
1958 and in 1959 they drilled 8 holes on the showing.  An EM survey
was done on the showing in 1958.  In 1966, more geophysical surveys
were completed over the showing as well as more drilling in the
showing vicinity by Indian Mountain Metal Mines Ltd.  No further
work was completed on the area until 1992 when Taiga Consultants
Ltd. on behalf of Royal Oak Mines, Asamera Minerals Inc. and Nebex
Resources Ltd. did an EM survey over the showing.
The Plex Lake showing is a CANMINDEX showing and is found on the
map 1198A as a cp occurrence.  No mention of this showing is made
in any assessment report.
The Susu Lake North showing is a canmindex showing located on the
COTTONGRASS Claims owned by BHP-Utah Mines Ltd. in the late 1980s.
They are located on the maps in assessment reports 082714 and
083069 but no mention of the showing is made in the written portion
of the reports.  The showing is considered a reconnaissance showing
and is recorded from the assessment report maps with an assay
result of 2859 ppm of Cu.
The 5 Mi West of Susu Lake showing is a CANMINDEX showing.  It is
located on the GSC 1198A map as a chalcopyrite occurrence and is
covered by ground geophysics in assessment report 017125.
The Brislane Lake-1 showing is defined by five grab samples taken
by Lebel Oro Mines Ltd. from the Indian Mountain Lake area.  The
area is within the Slave Structural Province, Archean in age.  The
samples returned assay results of 0.75% Cu, 0.65% Cu, 0.23% Cu, 2.
35% Cu, and 0.27% Cu.
The Brislane Lake-2 showing is defined by a single grab sample from
the Indian Mountain Lake area.  The sample is part of the Slave
Province, Archean in age.  Assay results are given as 0.03 oz. Au
and 0.45% Cu.
Regional The BRI 8 showing is situated within the Indian Mountain
greenstone belt which is mainly Archean Supracrustal rocks.
plutons of closely related age.  Property The BRI 8 showing lies in
the south-central part of the property and was prospected for
copper/gold occurrences.  A quartz diorite or tonalite intrusion
underlies this area of the property and is usually massive, medium-
to coarse-grained, creamy buff, and composed of quartz, feldspar,
biotite and hornblende.  The tonalite is seen to intrude the mafic
volcanics of the area.    Showing  The mineralization of the BRI 8
showing is in well fractured, altered quartz diorite.  It occurs as
chalcopyrite and gold with minor pyrite and pyrrhotite.  The
showing was explored in the 1950s by four trenches and smaller pits
which were dug and blasted on a series of parallel mineralized
fracture zones.  In 1992, in a joint venture between Royal Oak
Mines, Asamera Minerals and Nebex Resources, 16 samples from frost-
heaved boulders and the old trenches were taken.  Anomalous copper
values ranging from 912 ppm to 3.42% over narrow widths were
reported.  Two samples also returned anomalous gold values of 0.086
oz/t Au and 837 ppb Au.
Regional The Taco Island showing is situated within the Indian
plutons of closely related age.  Property The Taco Island showing
lies in the south part of Brislane Lake. The property was
prospected for copper/gold occurrences.  Most of the east half of
the island is underlain by hornblende-cummingtonite-biotite-garnet
schist while the west half is underlain by a hornblende schist.
Two narrow lenses of diopside-bearing rocks occur in the centre of
the island and near the north tip.    Showing  The mineralization
of the Taco Island showing is in two different lithologies - in the
diopside-garnet skarn and in the hornblende-cummingtonite-biotie-
garnet schist. The mineralization occurs as disseminated blebs and
fine stringers of pyrrhotite, pyrite and chalcopyrite.  In 1992, in
a joint venture between Royal Oak Mines, Asamera Minerals and Nebex
Resources 8 chip samples from higher grade sulfide occurrences on
the island were taken.  The best copper values reported were 5.58%
Cu over 0.6 m and 5.69% Cu over 1.0 m.  Anomalous gold values also
reported were 147 ppb Au and 740 ppb Au.
This is a CANMINDEX showing located as an occurrence on the Mineral
Occurrence Overlay Map 75M02.  No mention of this showing is made
in any assessment report or government report.
The BRI 6  showing is represented by 11 grab samples taken from
mafic volcanics south of Brislane Lake.  The volcanics are part of
the Indian Mountain greenstone belt and are Archean in age.  The
assay results for the grab samples ranged from 4274 ppm Cu over 0.
60 m to 7.06% Cu over 1.10 m.
The BRI 3  showing is a reconnaissance showing represented by 4
grab samples taken from mafic volcanics north of Brislane Lake.
The volcanics are part of the Indian Mountain greenstone belt and
are Archean in age.  The assay results for the grab samples ranged
from 2832 ppm Cu over 0.50 m to 2.09% Cu over 0.40
m
This showing is a CANMINDEX showing and is located as an occurrence
on the Mineral Occurrence Overlay Map 075M02.  No mention of this
showing is in any assessment report or government report.
This showing is a CANMINDEX showing and is a copper occurrence on
the Mineral Occurrence Overlay Map 75M02.  No mention of this
showing is made in any assessment report or government report.
The BRI 5  showing is represented by 8 chip samples taken from
mafic volcanic frost heave boulders north of Brislane Lake.  The
volcanics are part of the Indian Mountain greenstone belt and are
Archean in age.  The assay results for the grab samples ranged from
2806 ppm Cu over 0.80 m to 2.41% Cu over 0.70 m.
The JUF showing is a urainium occurrence in the Herriman Lake area.
Found within a biotite schist within granitic rocks, two samples
assayed 0.033% and 0.15% U3O8.   The showing was discovered prior
to 1952 by J. Woolgar and no further work on the showing has been
recorded since.
Record derived from the Canadian Mineral Occurrence Index
(CANMINDEX) of the Geological Survey of Canada.  Administrative
Region:  District of Mackenzie.  Showing is located 0.5 miles west
of Susu Lake.  The only records of the showing are from GSC map
1198A in which it occurs as a rusty zone with pyrite and pyrrhotite
and on the Mineral Occurrence Overlay 75M/02 in which it is shown
as a copper prospect.
The COTTONGRASS Cu showing is defined by a single grab sample from
Archean rhyolites in the Indian Mountain Greenstone belt.  The
rhyolites have been metamorphosed to granulite facies and are in
contact with quartz-biotite schists where the mineralization is
apparent.  The sample assayed 2580 ppm Cu.
The Susu Lake West 2 showing is a canmindex showing and is only
recorded on the Mineral Occurrence Overlay map as a copper prospect
showing.  No mention of this showing was found in any  assessment
reports or papers.
Regional The HO 16 showing is situated within the Indian Mountain
pyroclastics, and associated dykes and sills.  The rocks of the
Showing This showing is defined by 3 drill holes with a combined
total of 992 feet which intersected narrow bands of chalcopyrite,
sphalerite and pyrite in sheared dacite-andesite volcanics.  Best
intersections were 1.04% Cu and 1.02 oz/ton Ag over 2 feet and 0.
86% Cu over 4 feet.
Exploration The area in which the HO 16 claim lies was first staked
in 1949 by the McAvoy Option Group.  In 1959, three drill holes
were drilled to a depth of 992 feet.  No other work has been
performed on the showing, however in 1992, a joint venture between
Royal Oak Mines, Asamera Minerals and Nebex Resources did some
reconnaissance sampling nearby.
Regional The Pb No. 5 showing is situated within the Indian
total of 180 feet which intersected small amounts of chalcopyrite
in a rhyolite volcanic enclosed in a sediment.  No assay results
have been recorded.  Exploration During the winter of 1950, Captain
Yellowknife Gold Mines Ltd. drilled three diamond drill holes on
the PB 5 claim east of Indian Mountain Lake.
Regional The FLO showing is situated within the Indian Mountain
Showing The FLO showing is on the west of the northern part of
Brislane Lake, owned by J. Herriman in 1956.  In November of that
year a hole was drilled to a depth of 501 feet where chalcopyrite
and pyrite were observed within a narrow quartz vein.  No other
work has been completed on the showing although in 1992 a joint
venture between Royal Oak Mines, Asamera Minerals and Nebex
Resources did reconnaissance sampling in the immediate vicinity.
The Kennedy Lake West prospect is one of three related volcanogenic
massive sulphide occurrences situated in the Indian Mountain
greenstone belt in the southern Slave structural province. All
stratified rocks have been mapped as belonging to the Archean
Yellowknife Supergroup. The base of the stratigraphic sequence in
the vicinity of the deposits comprises a series of mafic tuffs with
minor, massive and pillowed mafic flows. The bottom of this unit is
tuff breccia.  The stratigraphic succession is completed by
greywackes and argillites. All stratified rocks have been
metamorphosed to middle amphibolite facies.  Mineralization of the
Kennedy Lake West prospect occurs as chalcopyrite with minor
amounts of silver and sphalerite.  The chalcopyrite is associated
with amphibole and garnet rich bands of the volcanics and is
disseminated in nature.  The mineralization can be traced
discontinuously over 2,000 feet between BB Lake and Kennedy Lake.
Pyrrhotite and pyrite are associated with the chalcopyrite in the
low grade sections at approximately a 1:1 ratio.
The Kennedy Lake West prospect is located on the VOO claims which
were first staked by James McAvoy in 1951.  In 1952, 6 diamond
drill holes were drilled on the VOO claims totalling 2,987 feet.
In 1959, trenching was carried out and 757 feet were drilled in 10
holes.  In 1965, Indian Mountain Metal Mines Ltd. located an
anomaly under Kennedy Lake which they drilled into in 1966.   The
drilling intersected a zone of low grade disseminated chalcopyrite
up to 120 feet wide.  This Kennedy Lake West copper zone has been
estimated to contain 1,000,000 tons grading 0.90% Cu over a length
of 835 feet.    In 1966, Indian Mountain Metal Mines Ltd. optioned
the VOO claims and drilled 9 holes and intersected the westward
extension of the copper zone.  The claims subsequently lapsed and
the ground was restaked by K. J. McDonald in May 1972 and later
that month transferred to Indian Mountain Metal Mines Ltd.
Exploration work included geological mapping and a ground EM survey.
Channel samples averaged 0.5% Cu and 0.94 oz./ton Ag over a width
of 25 feet.    In 1974, a tonnage figure for the Kennedy Lake West
zone was reported as 1,500,000 tons grading 0.62% Cu, including a
higher grade core of 612,000 tons grading 1.12% Cu.  In 1979,
Indian Mountain Metal Mines Ltd. amalgamated to form Initiative
Explorations Inc.  The property was then optioned off to Domego
Resources Ltd. in the early 1980s, who still held the claims in
summer 1998.
This VOY showing is from Mineral Occurrence Map 75M02 as a copper
prospect and was converted as a CANMINDEX showing.  No mention of
this showing is found within any other assessment report.
Regional The Benny Bay Zone showing is situated within the Indian
Showing The Benny Bay Zone is defined by two holes drilled by
Indian Mountain Mines Ltd. in 1974 which intersected a zinc rich
zone.  Sphalerite with pyrite and pyrrhotite were seen within a
narrow stratiform zone within the upper calcareous fragmental
member of the felsic sequence.  The best reported assay value from
the two holes was 7.9% Zn over 37 cm. No other work on the Benny
Bay Zone has been recorded since the 1974 drilling, although in AR
083129 a summary of the zone is stated.
Regional The Northern Zinc Zone showing is situated within the
Indian Mountain greenstone belt which is mainly Archean
Supracrustal rocks.  Composed of volcanic and sedimentary rocks, it
is as much as 15 miles wide and extends 40 miles north from Great
Slave Lake.  The belt is bound on the east and west by granitic and
migmatitic rocks but has a core of relatively low grade metamorphic
rocks(Heywood and Davidson 1969).  The belt is seen to lie on
deformed granitoid rocks in some places and in others to be
intruded by granitic plutons of closely related age.  Property
Rocks in the property area are almost entirely of volcanic origin
and consist of flows, pyroclastics, and associated dykes and sills.
The rocks of the property have been folded, striking approximately
north-south, and are crosscut by a fault that is directly north of
the showing.    Showing Mineralization is found within quartz-
carbonate stockworks in volcanic flows and occurs as sphalerite,
chalcopyrite and lead.  Its occurrence can be massive, disseminated
or as blebs within the host rock.  Garnets occur with the
mineralization as well as some minor pyrrhotite, pyrite and silver.
Assay results from 2 holes drilled 180 m apart along strike,
intersected respectively 7.3 m averaging 7.53% Zn and 4.88 m
averaging 4.83% Zn.
zone in 1948, just south of the Northern Zinc Zone showing.  The
area was staked in 1957 and 1958 by the McAvoy Option Group.  The
property was then optioned off to Mount Wright Iron Mines Company
Ltd. in 1958 and in 1959 they drilled 4 holes on the showing.  An
geophysical surveys were completed over the showing as well as more
drilling by Indian Mountain Metal Mines Ltd in 1974.  No further
work was completed in the area until 1992 when Taiga Consultants
Resources Ltd. reported values from two drill holes from previous
work done on the claim in 1974.
Regional The No. 2 Copper Zone  showing is situated within the
the showing.    Showing Mineralization is found within volcanic
flows and occurs mainly as chalcopyrite, sphalerite and silver.
Its occurrence can be massive, disseminated or as blebs within the
host rock.  Garnets occur with the mineralization as well as some
minor galena, pyrite and arsenopyrite.  Assay results from 15 drill
holes with a total of 3306 feet drilled, range from 0.30% Cu over
12 inches to 6.15% Cu over 48 inches and 0.30% Zn over 36 inches to
1.26% Zn over 48 inches.  The silver also had assay results but no
zone in 1948, just south of the No. 2 Copper Zone showing.  The
Ltd. in 1958 and in 1959 they drilled 15 holes on the showing.  An
drilling by Indian Mountain Metal Mines Ltd.  No further work was
completed on the area until 1992 when Taiga Consultants Ltd. on
behalf of Royal Oak Mines, Asamera Minerals Inc. and Nebex
No claims found to be associated with this showing, quite possibly
a GSC mapping find.  No exploration company assessment report was
found covering the showing.  The showing was converted from
CANMINDEX.
The Brislane Lake showing is a CANMINDEX showing.  No record of
this showing is made in any assessment report.
In 1966, Precambrian Mining Services, on behalf of Anglo United
Development Corporation and (according to NMI) Northgate
Exploration Limited, conducted a regional exploration program known
as Project Circle in the Camsell - Rivett Lakes greenstone belt,
focussed on the volcanic-sediment contact. Reconnaisance HLEM and
magnetic surveys, followed by geological mapping in areas of
detected conductors, revealed a number of targets deemed worthy of
follow-up. Not all surface sampling results are provided in the
submitted Assessment Reports. Five drill holes in 1967 tested
targets at the NW end of Lac Sans Disant, for which there is no
surface information in the Reports, while the C-6, C-3 and P-2
targets, deemed the most interesting in conclusions to the final
1966 report, were not drill-tested.  The Q4 occurrence is defined
by one drill hole which cut 0.26% Zn over 3 feet, and a number of 3
ft and 6 ft sections which assayed 0.10 and 0.15% Zn. Another hole
testing conductor O1, about 500 m to the NE, yielded a 10 ft
section of 0.10 % Zn.
The Tip and Nut are possibly a restaking of the Roc claims (NMI
075M05CU 003).  Regional: The property is located near the center
of a narrow 70 km long NNE trending belt of Archean Yellowknife
Supergroup, volcanic and sedimentary rocks within the Slave
Province.  The belt, known as the Camsell Lake Belt forms the
eastern limb of a synclinal fold cored by Archean biotite-muscovite
granites.(GSC map 738-A)  Property: The property lies on a contact
between meta-volcanics to the east, and meta-sediments to the west.
The volcanics on the property include mafic to felsic volcanic
cycles younging to the and including intervals of tuff, interflow
sediments and sulphidic exhalites and rhyolite domes.  Overlying
the volcanics are typical Yellowknife group amphibolite grade
turbidites.  The showing occurs 100 feet from a shear zone near the
volcanic sediment contact.
Showing: The TIP showing on the KIM #1 claim was discovered in 1949
by prospectors for a syndicate headed by W.J. McDonough.  The
property was subsequently staked by a number of individuals and
companies including Tailsman who drilled the showing in 1971
finding gold bearing vein up to f feet thick.  In 1984 J. R.
Woolgar did a soil chemistry and VLF survey over the property as
well as mapping and chip sampling.  The Tip gold showing is
comprised of a mineralized quartz vein in a chlorite, amphibole
schist striking at 35 degrees and  dipping steeply. The vein which
is 20 cm wide on surface and up to 1 m  wide in drilling is exposed
over 35 meters of trenching and has locally abundant pyrite with
minor arsenopyrite, chalcopyrite, galena, and visible gold.  Trench
samples graded up to 9.082 oz/t Au over 15 cm, and one grab sample
ran 35.55 oz/ton.  The host amphibolite did not carry gold. The
host rock to the east of the vein consists of meta-basalts and meta-
andesites with locally well developed pillows.  The host rock to
the west consists of meta-sediments which are not exposed. Several
other gossans, shears and quartz veins have been sampled on the
property with no notable results.
Regional: The SAN property was located in the southeastern Slave
Province, near the center of a narrow, 70 km long, NNE trending
belt of Archean volcanic and sedimentary rocks belonging to the
Yellowknife Supergroup.  This belt, known as the Camsell Lake Belt,
forms the eastern limb of a synclinal fold cored by Archean biotite-
muscovite granites (GSC Map 738-A).  Showing Area: The area is
underlain by rhyolite, dacite, and slaty tuff of amphibolite facies.
An EM survey was conducted in the spring of 1966 by Precambrian
Mining Services for Anglo United and Northgate Exploration.  Later
that summer the anomolies and pre-existing trenches were drilled.
The zone of interest is approximately 1 km long and 20 m wide
(Northern Miner, Aug 25, 1966, p3).
Showing: Anomoly C-3 consists of a warped sulphide lens striking
ENE and dipping steeply to the north in dacite and slaty tuff.  The
very fine grained laminated sulphides include po and lesser sph,
with py. nodules and some cpy. The C3 zone drilling assayed up to 0.
4%Cu and 2.4% Zn. Anomoly C-7 contains very fine grained po., with
coarse fracture fillings of po., in a rhyolite outcrop. The C7 zone
drilling assayed up to 1.0% Zn and 0.5% Cu. Anomoly C-6 is located
near the contact of an erregular north striking diorite dyke which
dips 55 degrees east. The mineralized zone contains po., cpy. and
pentlandite.  The C-6 drilling assayed up to 1.03% Ni. and 0.85% Cu.
Regional: The LEN showing is situated within the Camsell Lake Belt
of volcanic and sedimentary rocks of the Archean Yellowknife
Supergoup of the Slave Province.  The 80 km long Camsell Lake Belt
is a north east extension of the larger Campsell River belt.
Property: In 1947 Burgess-Yellowknife-Kirkland Mines Ltd. drilled 8
diamond drill holes on the property for a total of 2009 feet.  The
results were evidently disappointing and no further work was done.
No assays are available.  In 1962 the property was re-staked bu A.V.
Giauque and J.E. Sullivan who did geophysics and trenched the best
of the conductors.  Apparently visible gold was seen and one of the
trench samples graded .07 oz/ton Au.  Showing: Drill logs and
regional mapping show the host to be a sheared, locally feldspar
porphyritic, andesite with quartz veining and up to 1% pyrite,
pyrrhotite and chalcopyrite. A site visit by W.R.A. Baragar however
described a quartz vien in a quartz feldspar porphyry interlayered
with meta-basalts of the Yellowknife group(GSC paper 63-9).  The
sources did agree that the main showing consisted of a less than 1
foot wide quartz vein in a massive sheared porphyritic volcanic
extrusive. The showing was first drilled in 1947 but the assay
results were not included in the assessment report.  It may be
assumed that no sygnificant gold values were detected. Geophysics
and trenching on the showing in 1962 showed poor results however
one sample graded .07 oz/ton Au, and another had 0.6% copper and 0.
3% nickel.
Regional: The property is located near the center of a narrow 70 km
long NNE trending belt of Archean Yellowknife Supergroup, volcanic
and sedimentary rocks within the Slave Province.  The belt, known
as the Camsell Lake Belt forms the eastern limb of a synclinal fold
cored by Archean biotite-muscovite granites.(GSC map 738-A)
Property: The property lies on a contact between meta-volcanics to
the east, and meta-sediments to the west.  The volcanics on the
property include mafic to felsic volcanic cycles younging to the
west and including intervals of tuff, interflow sediments and
sulphidic exhalites and rhyolite domes.  Overlying the volcanics
are typical Yellowknife group amphibolite grade turbidites.
Showing: This showing was discovered by Nebex resources in 1993.
The Asp Zone is a set of frost heaves near an outcrop of finely
laminated mafic and felsic tuffs and wacke with minor somewhat
bleached mafic volcanics. A one metre band of massive amphibolite
with adjacent rusty shears crosses the centre of the outcrop.  The
actual gold bearing frost heaves about 40 metres SSW (along strike)
of the outcrop are of a felsic or siliceous rock with quartz
veining and up to 5% fine grained disseminated aspy. in  rusty
bands.  Local lithologies suggest that this could be the sulfide
facies of an iron formation.
Showing: This polymetalic showing was discovered by Nebex Resources
in 1993. Prospecting located rusty, sulphidic boulders along a 500
m long trend roughly coinciding with the upper felsic/metasediment
contact near the southeast shore of Old Conoe Lake.  Sample 37711
(4.8 g/t gold) was taken from a boulder of probable felsic tuff
with quartz gal., sph., and cpy. Other samples of felsic float
contained py. and po. mineralization.  The area is covered with
glacial overburden. Of the 4 samples taken the highest metal assays
were 4880 ppb Au, 46 ppm Ag, 2.3% Pb, 1.17% Zn, and 0.122% Cu.
Nebex took 6 more samples on the Canoe grid in 1994 with the
highest gold value being 110 ppb.
in 1993. The WK grid on the Brian 5 claim covers a package of north
striking mafic volcanic flows, mafic crystal tuff and interflow
sediments.  Central to this package is a 20 m wide zone of
intensely carbonitized mafic volcanics.  The altered zone contains
abundant quartz-calcite stringers and veins with local py., po. and
cpy.  The basalt hosted WK vein is exposed over 5 m, and up to 1 m
in thickness.  It consists of white quartz with traces of py., cpy.
and up to 7.1 ppm silver.  Five copper assays between 0.25% and 0.
8% ppm were obtained from the WK vein and a gossan, also in basalt
80, m SSW of the WK vein.
Capsule
Geology
Showing is nothing more than the presence of chalcopyrite in a
gabbro sill, noted on a map.  The Canmindex record descibes it as
chalcopyrite grains and masses, but there is no indication of this
on the map.
The Ellice River Area lies within the northeastern portion of the
Archean Slave Structural Province. The region is bordered by the
Aphebian age Bear Structural Province to the west, and the Rae
Structural Province to the east. The principal underlying
supracrustal rocks belong to the Archean Yellowknife Supergroup and
consist mainly of volcanics and metasediments. Archean intrusive
and metamorphic rocks also underlie the region. Early Proterozoic
(Aphebian) clastic sedimentary and carbonate sequences of the
Goulburn Group unconformably overlie the Archean rocks locally.
Intrusive rocks of Hudsonian age and younger diabase dykes crosscut
the older lithologies.  The Ellice River Area and nearby Boot Lake
Area (076GNE0010) are within the Back River region. The Yellowknife
Supergroup in the property area is divided informally into three
major sequences.  The Back Group is the lowest sequence and is
comprised of felsic to intermediate flows, tuffs and breccias. The
Hackett River Group overlies the Back and consists of  volcanic
flows that range from felsic to mafic, as well as tuffs and
chemical sediments. The uppermost sequence is the Beechey Lake
Group, comprising turbidite sediments, greywacke, mudstone and iron
formation. Recent mapping by the Geological Survey of Canada
suggests that the Hackett River and the Back volcanic belts, which
are generally spatially separate, may be coeval in their upper
parts (Williamson and Olson, 1990).  At least four periods of
deformation have affected the Yellowknife Supergroup. Metamorphic
grade in the Back River Region ranges from sub-greenschist to upper
amphibolite facies.  Three periods of iron formation deposition
have been identified within the Back and Beechey Lake Groups
(Chandler et al, 1992). In the property area, iron formations are
believed to be equivalent stratigraphically to the uppermost iron
formations in the Beechey Lake Group.
The Beechey Lake Group in the Back River region are isoclinally
folded greywackes, siliceous greywackes and mudstones that are
interbedded with iron formation and are steeply dipping. The iron
formation consists mainly of magnetite and chert and is of the
oxide variety. Subordinate amounts of silicate iron formation are
also present (Williamson and Olson,1990).  The Beechey Lake Group
greywackes have been intruded by sill like bodies of Archean
felsite. Throughout the Ellice River area, numerous Helikian
Mackenzie Diabase gabbroic dykes strike northwesterly and intrude
the Archean rocks. The Beechey Lake sediments to the west have been
intruded by biotite-muscovite sills.   The sedimentary rocks and
the iron formations of the Beechey Lake Group as well as the gabbro
dykes have been cut by numerous north-northwesterly trending minor
faults. Along these faults, left lateral or right lateral
displacement ranges from 0.1 to 5.0 m.  The Beachey Lake Group
sedimentary rocks within the Ellice-Rooster-Boot Property have been
deformed into a broad Z shape extending from Scorpion Lake
(approximately 5 km to the SW)to Hammer Lake (approximately 11.5 km
to the SE). The Boot Lake granitic stock (located south of Boot
Lake approximately 7.5 km SSW), intrudes this stratigraphy but is
not believed to be responsible for the folding. The Z structure may
be the result of two regional scale fold systems (Chandler et al,
1992).  Mantling the Ellice River area, especially in the southern
and western parts, is a blanket of Quaternary glacial material.
The Ellice River Showing has two grids located on it. Map 1605.I-3
from assessment report 083053 is an excellent location map of the
area. The centre of the Ellice Creek grid is approximately  7.5 km
NNE from the Boot Lake camp. The Eagle grid centre is approximately
700 m SW of the Ellice grid and is an extension of same.  The
Ellice River oxide iron formations occur in a NNW trending belt
that is approximately 4.5 km long and 1.3 km wide. Silicate iron
formations two kilometers to the southwest occur in a subparallel
trending belt 3.8 km long and 0.9 km wide. The Ellice River Archean
rocks are overlain uncomformably by the Aphebian Goulburn Group
sedimentary rocks and the Bathurst Fault System terminates it to
the east (Williamson and Olson, 1990).   The Ellice River iron
formations are interbedded with greywacke, mudstone and quartzite.
Johnston et al (1985) describes two types of sulphidic zones found
within the Ellice River area iron formations. Toward the southeast,
pyrite, pyrrhotite +/- arsenopyrite make up 10% volume of the rock.
Toward the NW end of the iron formation, the sulphidic zones
contain one or more of the following: pyrite, chalcopyrite,
pyrrhotite, native copper, galena, malachite and azurite. The
sulphide and carbonate minerals are usually concentrated in
fractures within the iron formation in isolated occurances.  As of
1992, the best assay result for the Ellice River grid is 57.63 g/t
Au from a sample of oxide iron formation from a rubbly outcrop in
the vicinity of a fold nose.  A cobble of oxide iron formation with
10-15% pyrite assayed at 45.36 g/t Au but was not traced along
strike due to heavy overburden cover.
The Eagle Grid lies within the southwest corner of the Ellice River
Showing.  The Eagle gold occurrance on this grid (Williamson and
Olson, 1990) is hosted in a sequence of interbedded oxide and
silicate iron formations which are associated with continuous
moderate positive ground magnetic anomalies up to 30 m wide. The
anomally indicates an extention of the Eagle iron formation of 450
m. Good quality VLF-EM anomalies are coincident with the western
edge contact of the iron formations hosting the Eagle occurance. A
ground VLF-EM conductor with poor quality VLF-EM anomalies is
coincident with the north northwest striking positive magnetic
anomaly of the Eagle formation.  Less than 10% of the area within
the Eagle grid are outcroppings of Beechey Lake Group sedimentary
sequences of greywacke, siliceous greywacke and mudstone with
silicate and oxide iron formations and intrusive Helikian gabbroic
dykes. Where exposed, the Eagle oxide iron formation is
approximately 10 m wide and occurs within a 30 m wide sequence of
interbedded oxide iron formation, silicate iron formation and
greywacke. East of the Eagle occurance, silicate iron formations
ranging in widths less than 0.5 m to 2.0 m are interbedded with
greywacke. The gabbro dykes trend northwesterly through the grid
and range from 0.1 m to 25 m wide.  The predominant sulphides of
the oxide or silicate iron formations of the Eagle grid are pyrite
and pyrrhotite. Sulphidic zones within the iron formations contain
one or more of pyrite, pyrrhotite and arsenopyrite. The pyrite
occurs locally as disseminated crystals, and as massive aggregates
in vuggy vein quartz. Amphibole and chlorite rich silicate iron
formation contains up to 1 volume per cent of the rock of fine
disseminated pyrrhotite. Arsenopyrite occurs with pyrite,
pyrrhotite or both in oxide iron formation that contains up to 50
volume per cent vein quartz (Williamson and Olson, 1990).
Rock grab samples and chip samples taken in 1986 from the main
sulphidic zones at Eagle occurrence assayed up to 177.43 g/t  Au
and 5.52 g/t  Au across 1.0 m respectively. Follow up work in 1990
consisted of rock and composite grab samples collected to the
northwest and yielded assays up to 2.57 g/t  Au and 0.14 g/t  Au
across 0.3 m respectively (Williamson and Olson, 1990). In 1993 one
drill hole intersected 22 m of oxide iron formation at the Eagle
occurance. The most significant assay obtained was 1.75 g /t   Au
over 1.24 m core from an interval of quartz +/- carbonate with
pyrite,and trace amounts arsenopyrite and pyrrhotite.
The Trout Lake Showing lies within the northeastern portion of the
Archean (>2.5 Ga) Slave Structural Province. The region is bordered
by the Aphebian age Bear Structural Province to the west, and the
Rae Structural Province to the east. The principal underlying
the older lithologies.  The Trout Lake Showing and nearby Boot Lake
Showing (NORMIN ID# 076GNE0010) are within the Back River region.
The Yellowknife Supergroup in the property area is divided
informally into three major sequences.  The Back Group is the
lowest sequence and is comprised of felsic to intermediate flows,
tuffs and breccias. The Hackett River Group overlies the Back and
consists of  volcanic flows that range from felsic to mafic, as
well as tuffs and chemical sediments. The uppermost sequence is the
Beechey Lake Group, comprising turbidite sediments, greywacke,
mudstone and iron formation. Recent mapping by the Geological
Survey of Canada suggests that the Hackett River and the Back
volcanic belts, which are generally spatially separate, may be
coeval in their upper parts (Williamson and Olson, 1990).  At least
four periods of deformation have affected the Yellowknife
Supergroup. Metamorphic grade in the Back River Region ranges from
sub-greenschist to upper amphibolite facies.  Three periods of iron
formation deposition have been identified within the Back and
Beechey Lake Groups (Chandler et al, 1992). In the property area,
iron formations are believed to be equivalent stratigraphically to
the uppermost iron formations in the Beechey Lake Group.
felsite. Throughout the area, numerous Helikian Mackenzie Diabase
gabbroic dykes strike northwesterly and intrude the Archean rocks.
The Beechey Lake sediments to the west have been intruded by
biotite-muscovite sills.   The sedimentary rocks and the iron
formations of the Beechey Lake Group as well as the gabbro dykes
have been cut by numerous north-northwesterly trending minor faults.
Along these faults, left lateral or right lateral displacement
ranges from 0.1 to 5.0 m.  The Beechey Lake group sedimentary rocks
(including the oxide iron formations) within the Boot-Rooster-Ellis
property have been deformed into a broad Z shape the extends from
Scorpion Lake to Hammer Lake. Chandler et al (1992) postulate that
the Trout Lake iron formation joins the iron formation at Scorpion
Lake North. The Boot Lake granitic stock intrudes this stratigraphy
but Williamson 1991, believes that two regional scale fold systems
may be responsible for the structure (Chandler et al, 1992).
Map 1-P92.001 from assessment report 083153 is an excellent map of
the locations of the various showings within the Ellice-Rooster-
Boot Lake Area.  The Trout Lake iron formation strikes north to
northeast from the northern end of Tea Pond. It is bound by a
sequence of greywacke/mudstone to the east and to the west the area
is swamp and overburden. Proterozoic outliers of the Goulburn Group
outcrop approximately 800 meters north of Tea Pond.  The
predominant sulphides of the oxide or silicate iron formations of
Trout Lake are pyrite and arsenopyrite.  Oxide iron formation with
intense quartz  veins, chlorite, up to 20% pyrite and 0.5 - 2%
arsenopyrite was traced over a 150 meter strike length.
Arsenopyrite occurs as subhedral to euhedral rhombs, often in a
black, highly siliceous cherty material.  Chandler et al 1992.
Grab samples from oxide iron formation (1992) include gold values
of 30.45 g/t, 26.67 g/t, 18.51 g/t, 16.63 g/t and 15.09 g/t. Grab
samples from 1991 yeilded gold values of 8.88 g/t, 12.51 g/t and 7.
61 g/t.  The silicate iron formation is dark green and amphibole
rich and has numerous quartz veins and trace to 2% pyrite. Values
of 9.98, 6.41 and 7.95 g/t Au were returned from 3 samples. The
banding/bedding has a steep dip to the east (80-85 degrees).  No
iron formation was traced south of Tea Pond as this area is heavily
covered by swamp and overburden.
The Scorpion Lake North Area lies within the northeastern portion
of the Archean Slave Structural Province. The region is bordered by
the Aphebian age Bear Structural Province to the west, and the Rae
the older lithologies.  The Scorpion Lake North Area and nearby
Boot Lake Area (DB ID# 076GNE0010) are within the Back River region.
ranges from 0.1 to 5.0 m.  The Beechey Lake Group sedimentary rocks
within the Ellice-Rooster-Boot Property have been deformed into a
broad Z shape extending from Scorpion Lake (on the western shore)
to Hammer Lake (approximately 12.5 km to the SE). The Boot Lake
granitic stock (located south of Boot Lake approximately 5 km SSE),
intrudes this stratigraphy but is not believed to be responsible
for the folding. The Z structure may be the result of two regional
scale fold systems (Chandler et al, 1992).
Boot Lake Area.  The Scorpion Lake North occurance is in oxide and
silicate iron formation on the southwest shore of Scorpion Lake
that has been silicified and locally sheared. Southeast of Scorpion
Lake the sulphidic zone can be traced continuously for
approximately 110 m in outcrop and feldsenmeer before being covered
by overburden. To the northwest, the sulphidic zone is traced
discontinuously for about 1 km.  The predominant sulphides of the
oxide or silicate iron formations of Scorpion Lake North are pyrite
and arsenopyrite. Locally, pyrite and arsenopyrite have a combined
volume up to 20% and are disseminated in the siliceous iron
formation or are associated with alteration haloes adjacent to
quartz veins.  In 1989 rock samples collected from the main
sulphidic zone in the most western iron formation assayed up to 22.
49 g Au/tonne. In 1990 rock and chip samples from the main
sulphidic zone assayed up to 5.07 g Au/t and 0.72 g Au/t across 1.2
m respectively. From the easternmost iron formation, a rock sample
assayed at 12.17 g Au/t.  In 1991 two holes were diamond drilled
(one abandoned due to drilling problems). Two gold bearing
sulphidic zones were noted in the drill core. In hole 1T015 assays
of 1.87 g Au/t over 5.18 m core length and 2.26 g Au/t across 1.95
m core length. In hole 1T015A  an assay of 3.09 g Au/t over 2.76 m
core length was recovered.
The Scorpion Lake Area lies within the northeastern portion of the
the older lithologies.  The Scorpion Lake Area and nearby Boot Lake
Area (ID# 076GNE0010) are within the Back River region. The
Yellowknife Supergroup in the property area is divided informally
into three major sequences.  The Back Group is the lowest sequence
and is comprised of felsic to intermediate flows, tuffs and
breccias. The Hackett River Group overlies the Back and consists of
volcanic flows that range from felsic to mafic, as well as tuffs
and chemical sediments. The uppermost sequence is the Beechey Lake
ranges from 0.1 to 5.0 m.  Map 1-P92.001 from assessment report
083153 is an excellent map of the locations of the various showings
within the Ellice-Rooster-Boot Lake Area.
Scorpion Lake oxide and silicate iron formations are found within a
sequence of interbedded greywacke, mudstone and siliceous greywacke
to  impure quartzite. Locally, sulphides are spaially associated
with quartz veins, but the highest concentration of sulphides are
in zones in felsenmeer along the eastern and western margins of
outcrop. Based on geophysical data, Dufresne & Johnston (1987),
interpret that the Scorpion Lake iron formation is a continuation
of the iron formations within the west end of Boot Lake North.  The
iron formation is 12 to 14 m wide, is well banded and consists of
magnetite, chert, amphibole and minor chlorite.  Sulphides
associated with the Scorpion Lake iron formation, both the silicate
and the oxide, are spatially associated with siliceous zones or
quartz veins. Arsenopyrite is the most common sulphide and occurs
as medium to coarse grained disseminated euhedral crystals. Pyrite
and pyrrhotite occur as irregular patches or layers and as
disseminated fine to coarse grained crystals.  Exploration on the
Scorpion Lake Showing has included reconnaissance and grid mapping,
airborne and ground geophysical surveys, geochemical sampling and
drilling.  In 1991 and 1992, the Scorpion Lake iron formation was
drilled showing that gold bearing zones occur along the west and
east margins of the iron formation. DDH 92T024 intersected two
zones that assayed at 6.79 g Au/t over 1.07 m and 7.70 g Au/t
across 2.9 m respectively. Hole 92T025 tested the southern
extension and recieved assays of 2.41 g Au/t across 2.02 m and 6.55
g Au/t over 1.26 m.  Drill results show lateral and downdip
continuity to the mineralization.
The Boot Lake Area lies within the northeastern portion of the
the older lithologies.  The Boot Lake Area is within the Back River
region. The Yellowknife Supergroup in the property area is divided
The Beechey Lake Group in the Back River Region are isoclinally
formation consists mainly of magnetite and chert and are of the
also present (Williamson and Olson, 1990)  The Beechey Lake group
sedimentary rocks (including the oxide iron formations) within the
Boot-Rooster-Ellice property have been deformed into a broad Z
shape the extends from Scorpion Lake (approximately 3.4 km NW) to
Hammer Lake (approximately 9 km to the SE).  The Boot Lake granitic
stock intrudes this stratigraphy but Williamson 1991, believes that
two regional scale fold systems may be responsible for the
structure (Chandler et al, 1992).  Boot Lake oxide and silicate
iron formations are found within a sequence of interbedded
greywacke, mudstone and siliceous greywacke to  impure quartzite.
Sulphides are spacially associated with quartz veins, Pyrite is the
most common sulphide, followed by arsenopyrite and locally
pyrrhotite.   Map 1-P92.001 from assessment report 083153 is an
excellent map of the locations of the various showings within the
Boot Lake Area.
The Showing area is comprised of several gold occurrences. The
central location of the major occurrences (ie extensively sampled
or drilled) is as follows. The location is the approximate distance
from the Boot Lake Camp (located on the north shore of Boot Lake).
Chick Pond 2.7 km NW; Ayers 2.2 km NW; Aiomon 1.5 km NW; Aiomon
West/Poison Pond 1.9 km NW;  Boot 1.1 km NW and Grizzly 2.15 km to
the NW of Boot Lake Camp.  The Boot Lake Showing area has been
extensively mapped, prospected, sampled (both rock and till),
diamond drilled and has had ground and airborne geophysical surveys
completed on it.  Some highlights of diamond drilling and sampling
results from 1991 & 1992 are as follows:  Ayers:  One chip sample
assayed at 17.76 g/t Au, three felsenmeer samples assayed 2.64, 4.
80 and 5.69 g/t Au (1992). Drilling: In 1991, 8 holes were drilled
totalling 1076.25 m. In 1992, 706.22 m were drilled in 5 holes.
Highlighted drill results include: 7.27* (8.64) g/t Au over 12.55 m
core length; 11.98* (14.10) g/t Au over 5.85 m and 9.34* (11.61) g/
t Au over 7.61 m.              Aiomon: One hole was drilled for a
total of 50.90 m in 1991. The best gold value was 1.29 g/t over 0.
93 m.  Aiomon West/Poison Pond: Four holes were drilled in 1992 for
a total of 245.05 m 11.57 g/t Au across 1.66 m (true width) and 2.
35 g/t Au over 1.55 m (true width).  Grizzly: In 1991 4 holes were
drilled for a total of 215.80 m, the best result was 3.29 g/t Au
over 1.67 m    *Assay sample cut to 34.268 grams gold per tonne; (
)=Uncut assay results; Meterage is uncorrected width unless stated.
The Winter Showing lies within the northeastern portion of the
the older lithologies.  The Winter-Boot Lake Area is within the
Back River region. The Yellowknife Supergroup in the property area
is divided informally into three major sequences.  The Back Group
is the lowest sequence and is comprised of felsic to intermediate
flows, tuffs and breccias. The Hackett River Group overlies the
Back and consists of  volcanic flows that range from felsic to
mafic, as well as tuffs and chemical sediments. The uppermost
sequence is the Beechey Lake Group, comprising turbidite sediments,
greywacke, mudstone and iron formation. Recent mapping by the
Geological Survey of Canada suggests that the Hackett River and the
Back volcanic belts, which are generally spatially separate, may be
shape the extends from Scorpion Lake (approximately 8 km SE of the
Winter area) to Hammer Lake (approximately 6 km to the E).  The
Boot Lake granitic stock (approximately 400 m W) intrudes this
stratigraphy but Williamson 1991, believes that two regional scale
fold systems may be responsible for the structure (Chandler et al,
1992).  Map 1-P92.001 from assessment report 083153 is an excellent
map of the locations of the various showings within the Boot Lake
Area.
The Winter Showing area iron formations occur in three spatially
separate arcuate belts. North of Puppet lake, the easternmost belt
is 130 m wide. Within this belt, there are 3 separate beds of oxide
iron formation 15-20 m wide and tracable for 700 m along strike.
Coexisting are numerous thinner oxide and silicate iron formations.
North of Turtle Lake, the central belt can be traced 950 m along
strike and is up to 100 m wide. The western belt near Winter and
Caro Lakes has small interbeds of mudstone and greywacke and is 15
to 20 m wide but poorly exposed.  In 1991 twenty grab samples were
collected and assays ranged from less than 0.7 g Au/t to 13.27 g Au/
t.  Thin cherty iron formations host the Spinster gold occurance
within the westernmost belt of the oxide iron formation. The iron
formation is covered by Winter Lake in the southeast but can be
traced for 100 m to the northwest. At  this occurance, pyrite is
found up to 10 volume percent. Two assays returned gold values of 4.
18 g/t and 13.27 g/t. North of Puppet Lake another grab sample of
pyrite and arsenopyrite bearing iron formation yielded a value of 1.
85 g/t Au.  At Grass Pond, (gold occurance 4DHZ001), grab samples
from sulphide bearing amphibole chlorite iron formation assayed
from 0.1 g/t Au to 4.79 g/t Au. Detailed chip samples within the
iron formation had gold values up to 4.95 g/t Au across 2 m. North
of Puppet Lake another grab sample of pyrite and arsenopyrite
bearing iron formation yielded a gold value of 1.85 g/t.
The Rooster-Hammer Showing lies within the northeastern portion of
the Archean Slave Structural Province. The region is bordered by
the older lithologies.  The Rooster-Hammer Lake area is within the
shape the extends from Scorpion Lake (~11.5 km SE of the Rooster-
Hammer area) to Hammer Lake. The Boot Lake granitic stock (~6.8 km
W) intrudes this stratigraphy but Williamson 1991, believes that
structure (Chandler et al, 1992).  Map 1-P92.001 from assessment
report 083153 is an excellent map of the locations of the various
showings within the Boot-Rooster-Ellice Area.
The Rooster-Hammer Area is a composite of 5 occurences. These
include Rooster Lake, Hammer Lake, Fox Pond, Falcon Creek and
Falcon Creek North. Map #1605.I-3  from Assessment Report 083053
shows the location and relationship of these occurences. Most of
the Rooster-Hammer area oxide and silicate iron formations are
poorly exposed as there is up to 95% glacial cover. This area has
been subject to sampling, mapping, ground and airborne geophysics,
trenching and diamond drilling.   The Hammer grid is 800 m east
northeast of Rooster Lake. This is a poorly exposed east trending,
south dipping 30-50 m wide oxide iron formation with interbedded
greywacke, mudstone and felsic dykes. At least 3 north trending
gabbroic dykes cut this sequence. The sulphidic zone is traceable
along the north edge of the iron formation with up to 10% pyrite,
5% arsenopyrite and trace pyrrhotite. Sulphides are spatially
associated with obliquely crosscutting quartz veins up to 0.3 m
wide or in siliceous iron formation. In 1987 an arsenopyrite and
pyrite bearing oxide iron formation contained visible gold. In 1991
three drill holes intersected gold bearing zones. The best result
at Hammer was in hole 1T009 which had two gold bearing
intersections in oxide iron formation. The assays of the north zone
were 7.28 g/t Au across 5.35 m core, the south zone assayed at 7.54
g Au/t across 5.61 m core.
Falcon Creek North has a glacial cover of 95%. Generally the
sediments and iron formation are easterly striking but two
exceptions indicate that there is a south plunging synform. In 1991
one grab sample from a pyritic silicate iron formation boulder
assayed at 0.69 g/t Au.  Fox Pond oxide iron formations occur as
isolated outcrops with 95% glacial cover. The oxide iron formation
is within a sequence of quartzite and greywacke +/- mudstone that
is is folded into tight or isoclinal folds that plunge to the south
southwest. Pyrite is the most common sulphide with arsenopyrite and
pyrrhotite in trace amounts. When sulphides are present they make
up to 1% volume of the rock. Dark quartz veins from 1 to 20 cm in
width are present in the oxide iron formation. From 1986 sampling a
composite grab sample gave an assay of 0.58 g/t Au across 0.3 m and
a grab sample of 0.79 g/t Au.  The Rooster Lake easterly trending
oxide and silicate iron formations occur in two (locally three)
discrete beds and are cut by northwesternly trending gabbroic dykes.
Greywacke and mudstone are interbedded with the oxide iron
formation that range from 0.5 to 35 m in thickness and locally host
zones of amphibole and chlorite. These zones are spatially
associated with quartz veins and contain pyrite, arsenopyrite,
pyrrhotite and gold. From 1985 the best results of diamond drilling
were 4.91 g/t Au over a core length of 8.02 m, 7.62 g/t Au across 1.
56 m and 2.44 g/t Au over 6.92 m. In 1992 further drilling resulted
in assays of 7.07 g/t Au across 1.16 m true width, 5.47 g/t Au
across 5.59 m true width, 12.62 g/t Au across 1.16 meters true
width and 6.43 g/t Au over a true width of 0.89 m.
The Dumbo Lake Showing lies within the northeastern portion of the
the older lithologies.  The Dumbo Lake - Boot Lake Area is within
the Back River region. The Yellowknife Supergroup in the property
area is divided informally into three major sequences.  The Back
Group is the lowest sequence and is comprised of felsic to
intermediate flows, tuffs and breccias. The Hackett River Group
overlies the Back and consists of  volcanic flows that range from
felsic to mafic, as well as tuffs and chemical sediments. The
uppermost sequence is the Beechey Lake Group, comprising turbidite
sediments, greywacke, mudstone and iron formation. Recent mapping
by the Geological Survey of Canada suggests that the Hackett River
and the Back volcanic belts, which are generally spatially separate,
may be coeval in their upper parts (Williamson and Olson, 1990).
At least four periods of deformation have affected the Yellowknife
shape the extends from Scorpion Lake (approximately 3.5 km SW of
the Dumbo Lake area) to Hammer Lake (approximately 12.5 km to the
SE).  The Boot Lake granitic stock (approximately 7 km S) intrudes
this stratigraphy but Williamson 1991, believes that two regional
scale fold systems may be responsible for the structure (Chandler
et al, 1992).  Map 1-P92.001 from assessment report 083153 is an
The majority of the Dumbo Lake area is covered in overburden. The
oxide and silicate iron formations are interbedded with greywacke
and mudstone. The iron formations range in width from 1 up to 10 m
in width and strike NNW on the north and west side of Dumbo Lake.
To the south and east side of Dumbo Lake the strike is westerly.
Silicate or silicate-oxide iron formation is the most common type
of iron formation to the Dumbo Lake showing. Trace to 2% volume
pyrite and pyrrhotite are common but no arsenopyrite was noted.
The sediments of the Dumbo Lake rocks have been intruded by white
weathered felsites 600 m NE of Bow Lake and 600 m SW of Bow Lake. A
granitic sill up to 150 m wide is traceable for approximately 1.9
km trending NNW to the southwest of Bow Lake. As well two types of
gabbro dykes outcrop in the Dumbo Lake area, one nonmagnetic and
metamorphosed, the other magnetic and nonmetamorphosed.  The Dumbo
Lake area was mapped and sampled at a reconnaisance scale in 1986.
Of 16 rock grab samples taken, assays ranged from 0.07 g Au/t to 0.
86 g Au/t.
The Shell Lake showing lies within the northeastern portion of the
the older lithologies.  The Shell Lake - Boot Lake Area is within
area is divided informally into three major sequences. The Back
The Shell Lake showing is an 8 m wide poorly exposed oxide iron
formation that has a NW strike. Williamson et al, 1991 suggests
that this may be a continuation of the Falcon Creek North iron
formation (included in the Rooster-Hammer area showing) that is
located approximately 1 km to the SE.  Two samples of pyrite and
arsenopyrite bearing iron formation were assayed and yeilded assays
of: 7.61 g Au/t and 12.51 g Au/t.
The Boulder Pond showing lies within the northeastern portion of
the older lithologies.  The Boulder Pond area is within the Back
River region. The Yellowknife Supergroup in the property area is
divided informally into three major sequences. The Back Group is
the lowest sequence and is comprised of felsic to intermediate
also present (Williamson and Olson, 1990)  Figure 4 from assessment
report 083213 is a map showing the general locations of  various
showings within the Boulder Pond area.  The Boulder Pond iron
formation is a NNW striking belt of sediments at least 8 km long
and 1.5 km wide and is an extension of the George Lake iron
formation. Aphebian Goulburn Group sedimentary rocks overlay
approximately 25 km of the belt between George Lake and Boulder
Pond.  The iron formation at Boulder Pond is stratigraphically
equivalent to the Goose Lake and George Lake iron formations but
the Boulder Pond iron formation is spatially associated with
volcaniclastic units of intermediate to felsic composition which
are interbedded with greywacke, mudstone and iron formation. Howe
(1994) suggests that this association may infer
Geological exploration has been done within the Boulder Pond area
since 1983. This includes prospecting, mapping, sampling,
airborne(1985) and ground geophysical surveys, grid establishment,
and drilling. A highlight of same follows:  In 1983 three grab
samples were taken from sulphidized iron formation NW of Peace Lake
that  has a strike length of 12 m. These samples yielded gold
values of 3.82, 2.35 and 1.17 g/t Au with up to 30% pyrite and 15 %
arsenopyrite(Howe,1993).  At East Boulder Pond, (occurrence
4DHZ004) thick sequences of well bedded magnetite chert oxide iron
formation are interbedded with silicate iron formation/chloritic
mudstone chert.  Gold occurrences exist in the sulphide bearing
sections of oxide and silicate iron formations and are associated
with arsenopyrite and pyrite adjacent to or within quartz veining
in the iron formation. A gold bearing interval from iron formation
assayed at 5.44 g/t Au across o.5 m in 1984. In 1986 two further
occurrences were discovered in this area and grab samples assayed
at 35.56 g/t Au and 20.98 g/t Au. In 1987 a VLF-EM geophysical
survey was done but no further sampling.  The Porkchop occurrence
is approximately 335 m SE of the south end of Opener Lake. This
occurrence is within a pyrite bearing silicate iron formation,
consisting mainly of chert and chlorite and having a minimum width
of 2 m.  A frost heaved boulder assayed at 4.83 g/t Au in 1987, 200
m to the SW a pyrite bearing iron formation grab sample assayed at
7.47 g/t Au.  The Jaeger occurrence is SE of Opener Lake and is an
oxide iron formation that has a strike length of 120 m with
sulphidic zones that have both arsenopyrite and pyrite. This poorly
exposed area returned assays of 6.34 g/t Au, 1.80 g/t Au across 3.7
m and 6.24 g/t Au across 0.9m in 1987.
The Player occurrence is approximately 500 m NW of Humpback Lake.
This is a silicate iron formation consisting mainly of chert and
chlorite that is 0.9 m wide and very poorly exposed. In 1987 a rock
chip sample of an arsenopyrite-pyrite bearing section assayed at 10.
49 g/t Au across 0.9 m. 40 m along strike to the NW a pyrite
bearing grab sample yeilded an assay of 3.33 g/t Au.  The Humpback
occurrence is 360 m west of the north end of Humpback Lake. It is a
silicate iron formation with pyrite bearing chert and greywacke
that outcrops next to a gabbroic dyke. This occurrence is very
pooorly exposed. 1987 assays of the pyritic chert yeilded values of
70.56 g/t Au and 43.41 g/t Au across 0.9 m.  From 1988 to 1991 no
further field work was done on the Boulder Pond area. Exploration
resumed in 1993 when remapping  and diamond drilling took place in
the East Boulder Pond and Peace Lake areas.  Three diamond drill
holes were drilled to test the the oxide iron formations in an area
of numerous Archean felsic dykes in the East Boulder Pond area.
Howe (1993) notes that the
Assays from diamond drilling include 3.53 g/t Au across 1.2 m core
length, 7.03 g/t Au across 0.65 m core length and 7.01 g/t  Au over
5.85 m core length.  A fourth diamond drill hole was drilled to
test a fold closure north of Peace Lake. Sulphidized and quartz
veined oxidized iron formations were intersected in this drill hole.
One sample assyed 0.33 g/t  Au over 1.2 m but the remainder of the
samples assayed under 0.2 g/t Au.  In 1994 three more diamond drill
holes were drilled in the Boulder Lake area to test oxide iron
formation mineralization. Two holes were drilled on the west side
of Opener Lake, the other, to the NW of Humpback Lake. Highlighted
assays include: 3.02 g/t Au over 2.25 m core length, 2.78 g/t Au
over 2 m core length, 1.54 g/t Au over 0.75 m core length for DDH
94P009 (NW end of Opener Lake), 1.54 g/t Au over 6.15 m core length
(NW Humpback Lake), 1.37 g/t Au over 1.7 m core length, 2.07 g/t Au
over 1.1 m core length and 5.77 g/t Au over 1 m core length in the
DDH at the SW side of Opener Lake.
The Soi Lake showing lies within the northeastern portion of the
the older lithologies.  The Soi Lake area is within the Back River
informally into three major sequences. The Back Group is the lowest
sequence and is comprised of felsic to intermediate flows, tuffs
and breccias. The Hackett River Group overlies the Back and
The Vega gold occurrence (approximately 100 m south of Soi Lake) is
within an arsenopyrite bearing part of the oxide iron formation. It
exists in northern trending linear bands slightly west of the
eastern edge of the oxide iron formation. Arsenopyrite and pyrite
occur adjacent to quartz veins. Rock grab samples assay up to 18.48
g/t  Au.  Approximately 720 m south of Soi Lake a hornblende rich
silicate iron formation contains arsenopyrite, pyrite and
pyrrhotite. Grab samples assay up to 74.64 g/ t Au  (Dufresne &
Johnston, 1984).  A chip sample from at this site assayed 16.73 g/t
Au over 0.60 m. Within 20 m in either direction along strike the
sulphides deccrease to trace amounts only. A similar silicate iron
formation is found 500 m south which assays at 3.60 g/t Au across 0.
9 m.  For approximately 1.5 km south of the gabbroic dyke, silicate
iron formations continue. The sulphidic zones of these iron
formations are gold bearing but the iron formations are generally
less than 1 m wide and the sulphidic zones a few meters in length.
also present (Williamson and Olson, 1990)  Map 6601-143 from
assessment report #082115  shows the  locations of  various
showings within the Soi Lake area.  The Soi Lake iron formation is
a NNW striking belt of sediments that is an extension of the
Boulder Pond iron formation which is stratigraphically equivalent
to the Goose Lake and George Lake iron formations. Ground magnetic
data from 1987 indicates that the Soi Lake iron formation exists in
a regional sized isoclinal fold. South of Soi Lake the Vega oxide
iron formation is 70-80 m wide and extends 200 m south where it
terminates adjacent to a 60 m wide NW trending gabbroic dyke. This
termination may be due to a fold closure, this is indicated by
repetative outcrop scale isoclinal folds.
The Goose Lake showing lies within the northeastern portion of the
the older lithologies.  The Goose Lake area is within the Back
also present (Williamson and Olson, 1990)  Map 5602-70 from
assessment report #081975 shows the location of the Goose Lake area.
The Goose Lake showing is within a northwest plunging antiformal
closure. Gold zones appear axial planar to the fold structure and
reasonably continuous in nature. The mineralization is interpretted
to occur in three subparallel zones occupying the west limb, fold
nose and east limb of the fold structure. The deposit is completely
open down plunge and along the strike of the limbs(Chandler et al,
1992). The Goose Lake iron formation has a NNW strike and is at
least 8 km long and 1.5 km wide.  The Goose Lake Showing is a NW
plunging antiformal structure that is comprised of a sequence of
interbedded greywacke, oxide iron formation, sillicate iron
formation and mudstone. This sequence has been intruded by felsic
and gabbroic dykes. The Goose Lake iron formation is believed to be
stratigraphically similar to the George Lake iron formation.  The
Goose Lake mineralized zones occur in both the west and east limbs
of the antiformal structure as well as in the fold nose. Chandler
et al,1992 interprets them to be subparallel to the axial plane of
the fold and steeply dipping. Increased quartz veining,
silicification, the development of chlorite and sulphide
replacement of magnetite characterize the gold bearing zones. Three
subparallel but spatially distinct zones of higher grade gold value
occur in the west limb (West Zone), fold nose (Main Zone) and east
limb (East Zone).
Gold zones appear axial planar to the fold structure and reasonably
continuous in nature. The mineralization is interpretted to occur
in three zones subparallel to the axial plane of the fold occupying
the west limb (West Zone), fold nose (Main Zone) and east limb
(East Zone) of the fold structure. The deposit is completely open
down plunge and along the strike of the limbs(Chandler et al,1992).
The Goose Lake iron formation has a NNW strike and is at least 8 km
long and 1.5 km wide.  Increased quartz veining, silicification,
the development of chlorite and sulphide replacement of magnetite
characterize the gold bearing zones.   Oxide iron formations host
the gold bearing sulphidic zones. The sulphidic zones contain up to
8 volume percent euhedral arsenopyrite and 7 volume percent
disseminated and wispy pyrite. Near the sulphidic zones the iron
formation is chloritic, foliated and graphitic and cut by quartz
veins. Flanking the larger oxide iron formation, thin beds of
silicate iron formation are present in greywacke. These contain up
to 7 volume percent disseminated and wispy pyrite +/or pyrrhotite
which occurs adjacent to quartz veins. This silicate iron
formations are at least 10 m long and up to 0.75 m wide.
Exploration in the Goose Lake area commenced in 1984 with
reconnaissance prospecting. A rock chip sample collected at Goose
Lake assayed at 1.30 g/t Au across 2.3 m and a grab sample assayed
at 17.11 g/t Au (Johnston et al,1985).  In 1985, an airborne DIGHEM
geophysical survey, reconnaissance mapping, prospecting and
sampling was done over the area, one assay had a value of 4.40 g/t
Au.  Exploration in 1986 consisted of detailed mapping, sampling,
and ground geophysical surveys of magnetometer, VLF-EM and HLEM. A
till sample survey was also done within the Goose Lake area.  Of 25
rock samples collected gold assays ranged from less than 0.7 to 8.
67 g/t Au. Four samples assayed between 3.00 and 8.67 g/t Au, two
samples assayed from 0.5 and 3.0 g/t Au. Fifteen samples had an
anomalous gold value ranging from 0.15 to 0.34 g/t Au.  In 1987
infill grid surveying, prospecting, ground magnetometer and VLF-EM
surveys were carried out to extend and delineate the iron formation.
From 1988 to 1991 no field work was done on the Goose Lake area.
In 1992 till sampling, ground geophysics (magnetic, VLF-EM and
gradiometer) and diamond drilling of 19 holes totalling 2,729 m. A
total of 869 core samples were taken with numerous assays exceding
20 g/t Au (e.g. 77.86 g/t Au over 1.0 m and 127.44 g/t over 1.25 m).
In 1993 a detailed geophysical survey and a legal survey was
completed at the Goose Lake property.  In 1994 21 diamond drill
holes were drilled totalling 7473 m.
A press release from Kit Resources on 25 March 1998 announced that
a new resource estimate had been calculated based on a drill
program from 1997. Twelve drill holes on the Goose Lake target
produced the best grades and widths and the deposit remains open to
depth. The indicated resource is 1,896,000 tonnes at 10.53 g/t and
642,00 contained ounces gold. Kit  Resources state  they intend to
test for depth extension in the next phase of drilling as well as
advance the project to prefeasibility stage as market conditions
improve.
The Goose Neck showing lies within the northeastern portion of the
the older lithologies.  The Goose Neck area is within the Back
90% of the Archean rocks in the Goose Neck area are covered by
glacial material. The Goose Neck oxide iron formation exists in two
places along the shore of Goose Lake and is interbedded with
Beechey Lake Group greywacke and and mudstone. The iron oxide
formations are well banded and consist of magnetite, chert and
grunerite and 1-2 volume percent pyrite. The iron formation trend
north north-west and is approximately 5m wide. Airborne geophysics
indicate that the oxide iron formation is complwexly folded and
faulted.  In the TGL5b target area (map 6601-179 from assessment
report 082116)a poorly banded to massive, thin silicate iron
formation consists of grunerite, hornblende and chlorite and is
interbedded with greywacke and mudstone. Within the iron formation
sulphidic zones contain up to 10% pyrite.  In 1985 reconnaissance
mapping and prospecting yeilded one rock grab assay of 4.40 g Au/t
from a pyrrhotite bearing zone in greywacke. Bartkiewicz & Johnston
(1986) note that this sample was from a boulder that was found on
the oxide iron formation. An airborne geophysical survey was also
flown over the Goose Lake area in 1985.  1986 exploration included
prospecting, mapping at a 1:2000 scale and sampling. Of four
samples collected within oxide iron formation none were over 0.07 g/
t Au. In the TGL5b area, approximately 950 m SW of the Goose Lake
shore, a rock grab sample from a sulphide bearing zone in a
silicate iron formation assayed at 0.34 g/t Au.
The Goose Creek showing lies within the northeastern portion of the
the older lithologies.  The Goose Creek area is within the Back
Glacial material covers 55 to 85 percent of the Goose Creek area.
Ground and airborne magnetic data indicate that the iron formation
trends to the NW, is folded into a S shape, then continues to the
NW into the Llama Lake area where it becomes complexly folded. It
is then traced back to the Goose Creek area.  There is one main
area of interbedded oxide iron formation in the Goose Creek area.
The iron formation is interbedded with Beechey Lake Group greywacke
and mudstone. Thin silicate iron formations outcrop locally and
occur as pods and lenses that are 0.5 m or less in thickness. The
silicate iron formations consist mainly of grunerite with lesser
amounts of chert and chlorite and are poorly banded.
Exploration of the Goose Creek area commenced in 1984 with
reconnaissance prospecting and rock sampling based on positive
aeromagnetic anomalies from the 1968 Geological Survwey of Canada
(Bartkiewicz & Johnston,1986).  In 1985 geological mapping at a
scale of 1:10,000, prospecting and sampling were done. As well an
airborne geophysical DIGHEM survey was flown over the area.  Rock
grab samples from 1984 and 1985 range from 0.005 g/t Au to 0.70 g/t
Au (Bartkiewicz & Johnston,1986).  Exploration in 1986 included
detailed prospecting and mapping at a scale of 1:1000, sampling,
ground magnetometer, VLF-EM and HLEM surveys, as well,
reconnaissance prospecting and mapping were done on other areas of
the property.  14 rock samples collected and gold values range from
less than 0.07 to 2.67 g/t Au. Three samples assayed at 1.06, 1.71
and 2.67 g/t Au. Five samples had  anomalous gold content of 0.15 g/
t Au or greater, these include assays from 0.17 to 0.75 g/t Au. Six
of the eight rocks that assay between 0.17 to 2.67 g/t Au were from
a sulphidic zone in the oxide iron formation, the other three were
from silicate iron formation beds and lenses.   In 1987 a ground
magnetometer survey was completed at the Goose Creek area to better
define the poorly exposed and complexly folded iron formation.  In
1992 reconnaissance till sampling was done over the Goose Lake area.
In 1986, Target TGL5a was prospected and mapped at a 1:10,000
scale. All the sulphide occurrences were in subrounded boulders so
the source is unknown. One of the boulders (located approximately 0.
6 km east of Big Lake) was of silicate iron formation and had 1
volume percent pyrite. Of six samples taken, one assayed at 0.34 g/
t Au, all the others were 0.10 g/t Au or less.
The Llama Lake showing lies within the northeastern portion of the
the older lithologies.  The Llama Lake area is within the Back
assessment report #081975 shows the location of the Goose/Llama
Lake area.  Glacial material covers 80 to 90 percent of the Llama
Lake area. Ground and airborne magnetic data indicate that the iron
formation in the Llama Lake area is complexly folded.  Beechey Lake
Group greywacke and mudstone and quartzite, oxide and silicate iron
formations have a northwesterly trend. The well banded oxide iron
formations are generally 5 to 10 m thick and consist of magnetite,
chert and grunerite. The poorly banded grunerite, chert and
chlorite silicate iron formations occur as lenses or pods up to 0.5
m thick within greywacke and mudstone. Both types of iron
formations ontain sulphides and carbonates locally.
Sulphidic zones in both oxide and silicate iron formations are
spatially associated with quartz veins. The dominant sulphide is
pyrite, but arsenopyrite and pyrrhotite are also present locally.
Pyrite occurs in irregular patches and as disseminated crystals.
Arsenopyrite exists as medium grained disseminated crystals at or
near the margins of the quartz veins and is associated with pyrite.
Pyrrhotite occurs as disseminated fine grained crystals or as
irregular patches. Dufrsne and Johnston, 1987 note: In general,
rock samples that contain greater than one volume percent
arsenopyrite assay greater than 1.00 g/t Au. Rock samples that
contain pyrite or pyrrhotite or both assay less than 1.00 g/t Au.
A 2 m wide siliceous felsite dyke intrudes the greywacke
approximately 100 m north of Llama Lake. West of Llama Lake
(approximately 1.5 km), a granitic pluton intrudes the sediments.
Helikian gabbroic dykes ranging from 5 to 30 m in width exist
parallel to the trend of the iron formations and interbedded
sediments.  Reconnaissance exploration was conducted at Llama Lake
in 1984 and 1985. In 1985 a DIGHEM airborne geophysical survey was
performed as part of a larger regional survey.   In 1985 a gold
occurrence was discovered about 600 m SE of the southern tip of
Llama Lake in a sulphide bearing 0.5 m wide silicate iron formation
that was adjacent to a crosscutting quartz vein. A rock grab sample
from this sulphidic zone assayed at 4.10 g/t Au. The sulphidic zone
contained 10 volume percent pyrrhotite,5 volume percent pyrite and
2 volume percent arsenopyrite.  In 1986 a base line was established
and reconnaissance mapping and sampling were performed.
Three gold occurrences were discovered in  1986, each defined by a
single rock sample collected from sulphide bearing zones in
silicate iron formations less than 0.5 m wide. The sulphide zones
are adjacent to crosscutting quartz veins within the iron formation.
Two occurrences are west of Llama Lake, the other is to the
southeast.  110 m west of Llama Lake a grab sample from a sulphide
bearing zone assayed at4.15 g/t Au. This zone had 3-5% pyrite and 2-
3% arsenopyrite by volume.  200 m south of the above occurrence a
grab sample from another sulphie bearing silicate iron formation
assayed at 2.06 g/t Au. This zone had 2-3 volume percent pyrite.
500 m south of Llama Lake the third occurrence had a sulphide
bearing zone of 1-2 volume percent arsenopyrite and assayed at 1.30
g/t Au.  1987 exploration included prospecting, sampling, mapping
at a scale of 1:2000, and ground magnetometer and VLF-EM surveying.
One rock chip and 44 grab or composite grab samples were taken.
Three samples assayed between 0.50 g/t Au and 3.00 g/t Au, the
remaining assyed less than 0.5 g/t Au.  A gold occurrence was
discovered 135 m west of the north end of Llama Lake in a 0.5 to 1
m wide silicate iron formation that was pyrite and arsenopyrite
bearing. A rock grab sample assayed at 1.44 g/t Au. Samples
collected from bands of silicate iron formation that occur along
strike to the NW and SW of this occurrence assay up to 0.51 g/t Au.
80 m south of Llama Lake a gold occurrence within a pyrite and
arsenopyrite bearing oxide iron formation that is 10-15 m wide
assayed at 2.71 g/t Au. This iron formation is poorly exposed over
a strike length of 110 m. Arsenopyrite was found in only one
location but pyrite exists throughout.  In 1992 a reconnaissance
till sampling survey was carried out.
The Yava Showing, also referred to as the Agricola Lake deposit,
occurs within the Hackett River volcano-sedimentary belt which
comprises rocks of the Archean Yellowknife Supergroup. The Showing
is located near the top of the Hackett River Group, which typically
consists of a succession of fragmental rhyolites capped with basalt
flows and overlain by pillowed andesites. In the vicinity of the
Yava deposit, the pillowed andesites are largely absent, replaced
by a fragmental-rich sequence of dacitic ash flow tuffs overlain by
the main host unit of generally siliceous volcanics. The latter
includes massive, bedded, and glassy felsic volcanics interlayered
with chert, graphitic argillite, pyrite/pyrrhotite and limestone,
and is dominated by tuffs and lapilli tuffs near the deposit.
The main sulphide mineralization is found near the
base of the siliceous unit, and an alteration pipe/stringer zone
extends down into the underlying dacitic tuff. Sphalerite occurs in
a series of layers throughout a 95 metre stratigraphic interval in
the centre of the deposit, although the main mineralized beds are
found within an interval between 15 and 30 metres thick. Sulphidic
layers are thick and closely spaced in the central areas, and
thinner as well as more widely spaced toward the periphery. They
tend to be either pyrite or sphalerite-rich, with peak pyrite
concentrations generally underlying peak concentrations of ore
minerals (CIMM  Bulletin V73N815P143).                     There is
a vertical metal zonation, with successive layers from bottom to
top changing from chalcopyrite-rich to low-Fe sphalerite plus
galena, to argentiferous tennantite + sphalerite + galena, and
finally to high-Fe, argentiferous and auriferous sphalerite, the
lower half of this layer is an argentiferous pyrite layer.
Alteration associated with the deposit is not described in detail.
Chlorite and sericite are present and the host rocks are soda-
depleted and enriched in magnesium and iron.   Regionally, the host
strata are part of the steep to overturned limb of a major syncline.
Crenulations and small scale S and Z drag folds are present in
bedded rocks. Most of these small folds plunge steeply, at least
some of them to the south.  The Yava Showing was discovered by a
GSC regional geochemical survey program in 1972-3. Work done since
then includes geological mapping, geochemical sampling (water, soil
and rock), airborne and grid-based ground geophysics (gravity,
magnetometer, resistivity), and diamond drilling.  A total of 15
diamond drill holes were drilled on the Yava Showing over 2 years
for a combined footage of 3376 ft. In the first phase of drilling,
6 holes were drilled totalling 1295 ft. Five of the holes
intersected steeply dipping sulphide sections with zinc, lead,
copper, silver and gold anomalies. These sections include a
stratigraphic upper zone rich in zinc and silver, a composite zone
with layers of nearly massive sulphide rich in zinc, lead, silver
with significant copper and gold and, a stratigraphic footwall zone
containing copper stringers. AR 080465 states that the drilled
sections contain more than 4% Zn, 1% Pb, 1% Cu, 1 oz/ton Ag, 0.01
oz/ton Au or combinations thereof.
In the second phase of drilling, nine holes were drilled for a
combined footage of 2081 ft; four of these tested targets outside
the main zone.  Three of the five holes testing the main zone
intersected base metal sulphides: 5.2 oz/ton silver, 1.85% zinc
over 2.5 ft core length in one hole; 3.8% zinc, 0.24 oz/ton silver
over 2.8 ft. core length in another hole; and 6.5% zinc, 0.37 oz/
ton silver over 5.4 ft. core length, and 3.10% zinc, 1.7 oz/ton
silver, 0.02 oz/ton gold over 3.7 ft core length in a third hole.
The following conclusions were reached at the end of this drilling:
The Main Zone drilling extended the Main Zone mineralization over
an area 1500 feet long and 500 feet wide and to a depth of at least
300 feet below surface.  Detailed drilling is required to define
the exact nature and grade of the Main Zone.  Drilling on targets
outside the Main Zone intersected only traces of ore mineralization.
(Assessment Report 080538)  There is no indication of any further
work being done on the showing.  No further Assessment Reports were
filed and no mention is made of further work in the annual Mineral
Industry Reports put out by DIAND. Expenditures to the end of 1975
were sufficient to secure the property until 1984, at which time it
was taken to lease.
The Yava Showing has been cited in numerous references as having
drill-indicated reserves of 1,000,000 to 2,000,000 tonnes grading
3% Zn, 0.5% Cu, 0.5% Pb, 102.8 g/t (or 10%) Ag and 2 g/t Au. It is
difficult to determine what these figures are based on, and the
only conclusion which presents itself is that they are based on the
8 mineralized intersections of the 1974-75 drill program - or more
accurately, on speculation regarding these intersections. The
National Mineral Inventory (EMR Canada, Mineral Policy Sector)
gives separate grades for two sections of the deposit and a total
size of 1,250,000 tons, quoting a talk presented at the 1976
Geoscience Forum.  Since no work appears to have been done in 1976,
these reserve figures must be based on the 8 intersections
mentioned above and therefore do not meet any commonly accepted
criteria for definition as an ore reserve. The publication called
Canadian Mineral Deposits Not Being Mined in 1989 (EMR Canada,
Mineral Policy Sector) also gives reserve figures for Yava, quoting
a 1982 paper but giving 1976 as the date of the calculation.  Again
the only conclusion is that the figures are based on inadequate
information, possibly supported by frequent references to the Yava
massive sulphide deposit in various journal articles and other
publications.  Support for this view is found in an addendum to
Assessment Report 080538, in which  the results of the five 1974
drill intersections are discussed rather optimistically.  The
author interprets three zones and calculates average horizontal
widths, tons per vertical foot, and grade of each zone from these
five intersections, then goes on to say:  It is reasonable to
suppose that the M zone extends 100 feet north of Y3 and 200 feet
south of Y4. If this is so, the zone would contain 1 million tons
to an average depth of 300 feet, 2 million tons if the body reached
a depth of 600 feet.
This is the first mention of 1 to 2 million tons in available
sources. It is interesting to note that the deepest sulphides were
intersected at 290 ft below surface.  This Showing has been
assigned a Development Stage of Drilled rather than Resources
Calculated, in accordance with the conclusions reached above.
The George Lake area lies within the northeastern portion of the
the older lithologies.  The George Lake Area is within the Back
divided informally into three major sequences.  The Back Group is
felsite. These sills are generally 1-3 m wide with the exception of
one at the NW end of George Lake which is up to 130 m wide and 2.3
km long.   The sedimentary rocks and the iron formations of the
Beechey Lake Group as well as the Aphebian Goulburn Group sediments
have been cut by numerous NNW trending Helikian gabbroic dykes.
Approximately 50% of the Precambrian rocks of the George Lake area
are mantled by quaternary glacial material.  The metamorphic grade
of the Beechey Lake Group in the George Lake area is lower to
middle greenschist.  The George Lake area has been subject to an
increasing scale of exploration since 1982. The area has been
prospected, mapped, trenched, sampled and drilled as well as having
airborne geophysics and detailed ground geophysics done.   In the
George Lake area, iron formations within Beechey Lake sedimentary
rocks strike northwest. This 16 km long and 2.5 km wide iron
formation/sediment sequence has three major oxide iron formation
belts identified within it. These belts are: the George Lake belt,
the Fold Nose belt and the Lookout Hill belt.  Maps 6601-31 & 32
from assessment report 082117 show the three main belts as well as
the main mineral occurrences and their locations. All locations of
occurrences are taken from an approximate midpoint and located with
reference to the George Lake camp (GLC) which is on the SSW shore
of George Lake.
Gold exists in sulphide facies within oxide iron formations in
several areas in the George Lake area. Five deposits are
highlighted but there are numerous gold occurrences throughout the
area. Assays (from 1988) marked with an asterick are cut assays to
34.268 g Au/t.  The George Lake North deposit consists of Locale 1 -
Locale 1 North. Locale 1 North-Locale 1(approximately 1.2 km NW of
GLC) gold bearing sulphidic zone has a minimum strike length of
approximately 960 m, an average vertical extent of approximately
200 m and a true width of 3.7 m for intersections with a gold grade
times width product over 10 g*m. One drill hole intersected a zone
with a weighted average of 9.02* g/t Au over 10.53 m core length.
Locale 1 North (1.8 km NW of GLC) has two oxide iron formations
that are the steeply SW dipping limbs of a syncline. The SW limb is
gold bearing and ranges from 5 to 50 m wide. Gold in the oxide iron
formation is spatially related to quartz veins and the sulphidic
zones have abundant quartz and chlorite, up to 15% pyrrhotite and
lesser pyrite and arsenopyrite. Visible gold is present with
chlorite and sulphides within and near quartz veining.  The
Occurrence Lake deposit (formerly Locale 2, approximately 400 m SW
of GLC) has a gold bearing sulphide facies iron formation that
ranges from 2.72 to 18.77 m wide and strikes for 110 m. Mudstone
and greywacke beds are often intercalated with the iron formation.
Visible gold is associated with white vein quartz and arsenopyrite
veins which crosscut the iron formation. The best drill core result
from 1988 produced a weighted average of 4.9 g/t Au over 13.32 m
core length.
The Esker Pond deposit (formerly GH): The southwest oxide iron
formation (approximately 3 km S of GLC) has a gold bearing
sulphidic zone that has a minimum strike length of 240 m which
extends to a depth of at least 270 m below surface (average depth
of 120 m) and an average true width of approximately 4.9 m for
intersections with a grade times width gold value over 10 g*m. The
iron formation exists in a tight SE plunging syncline. Two drill
holes from 1988 gave weighted averages of 8.33 g/t Au over 13.65 m
core length and 17.91* g/t Au across 6.14 m core length. GH South
(2.5 km S of GLC)has an oxide iron formation within an isoclinal
syncline that contains pyrite, arsenopyrite and visible gold
associated with chlorite and quartz veining. The gold bearing
sulphidic zone has a strike length of at least 120 m in the NE part
of the iron formation. The highest weighted average obtained from
the 1988 drilling was 2.83 g Au/t over 15.27 m core length.  The
Slave deposit (approximately 1.2 km ESE of GLC) has thick oxide
iron formation as well as silicate iron formation, both are folded
and faulted. Gold exists in sulphidic zones which are spatially
related to quartz carbonate veins and usually contain chlorite.
Sulphides include pyrite and arsenopyrite. At Slave Central Fold a
drillhole intersected a zone which gave a weighted average of 10.
94* g/t Au over 10.14 m core length. At Slave Northern Folds, a
weighted average of 2.12 g/t Au over 10.55 m core length was
obtained.  The Lone Cow Pond deposit (approximately 3.8 km NW of
GLC) has a gold bearing zone within a siliceous iron formation and
auriferous chloritic greywacke that is interbedded with mudstone.
Within the sulphide facies arsenopyrite is found up to 30% volume
and pyrite ranges from 2-20% locally. White quartz veins 1-10 cm
are found within the iron formation and the greywackes.
The gold bearing zone has two high grade shoots, the larger one
plunges approximately 40 degrees NW with a true average width (for
grade times width over 10 g*m) of 3.4 m and a down plunge length of
430 m. The shoot ranges from 60-110 m in length perpendicular to
plunge axis. The highest gold weighted average from drilling in
1988 was 16.68* g/t Au over 8.23 m core length.  On March 24 1992
a public presentation to the NWT water board gave an undiluted
geological resource estimate for the five deposits of the George
Lake area as 3.1 million tonnes at a cut grade of 12.41 g/t gold to
a 300 m depth.   In 1996 when the George Lake properties changed
owners a news release from Arauco Resources Corporation  (July 2,
1996) stated that the George Lake property has over 100 surface
gold showings which assayed at over 10 g Au/t.  A 1998 press
release from Kit Resources Ltd. announced new resource estimates
based on a 21,000 m drill program conducted in 1997. Resource
estimate as follows: Locale 1: 1,228,000 tonnes @ 10.84 g/t, 428,
000 contained ounces gold Locale 2: 1,063,000 tonnes @ 11.62 g/t,
397,000 contained ounces gold Lone Cow Pond: 381,000 tonnes @ 10.74
g/t, 132,000 contained ounces gold GH: 228,000 tonnes @ 10.22 g/t,
75,000 contained ounces gold Slave: 176,000 tonnes @ 9.88 g/t, 56,
000 contained ounces gold  All of the mineralization is located
less than 300 metres below surface so a portion of the resource can
be mined by open pit. The resource was based on a cutof grade of 5
grams of gold per tonne. 93-95 percent of the gold would be
recovered using carbon in pulp milling techniques.  In July of 1998
an independent resource calculation was released in the NOrthern
Miner which expanded the size of the gold deposit. It is now
estimated to host 6.5 million tonnes averaging 9.76 g/t Au. The
increase is attributable to new inferred resources which total 2.22
million tonnes of 9.9 grams gold. The indicated resources total 4.2
million tonnes grading 9.8 grams gold.
The Rifle Lake area is in the SE section of the George Lake area
which lies within the northeastern portion of the Archean Slave
Structural Province. The region is bordered by the Aphebian age
Bear Structural Province to the west, and the Rae Structural
Province to the east. The principal underlying supracrustal rocks
belong to the Archean Yellowknife Supergroup and consist mainly of
volcanics and metasediments. Archean intrusive and metamorphic
rocks also underlie the region. Early Proterozoic (Aphebian)
clastic sedimentary and carbonate sequences of the Goulburn Group
unconformably overlie the Archean rocks locally. Intrusive rocks of
Hudsonian age and younger diabase dykes crosscut the older
lithologies.  The George Lake Area is within the Back River region.
the Fold Nose belt and the Lookout Hill belt.  Rifle Lake is in the
SW section of the George Lake area, on the Eastern side of the
Lookout Hill Belt, approximately 9.2 km from then George Lake Camp
(SW shore of George Lake).
Maps 6601-31 & 32 from assessment report 082117 show the three main
belts as well as the main mineral occurences and their locations.
The Rifle Lake area has been subject to a variety of exploration
activity since 1984 including reconnaissance and detailed
prospecting, sampling, mapping, geophysics (ground and airborne),
and diamond drilling.  The main concentration of exploration is in
the NW section of the Rifle Lake area on the western shore of Long
Lake where a thick oxide iron formation and a chlorite greywacke-
siliceous unit are well folded forming a SE plunging syncline. Fold
closures have an average plunge of 65 degrees SE. The oxide
formation is 12-60 m thick and is well banded with magnetite, chert,
grunerite and carbonate.   The chlorite greywacke-siliceous unit
is stratigraphically below the oxide iron formation. It has
discontinuous gold bearing siliceous layers and the iron formation
is up to 12 m wide. Fine grained disseminated pyrite is present in
the siliceous layers. In the siliceous-greywacke unit white quartz
and quartz carbonate veins to 1 m wide cut subparallel to parallel
to strike. Arsenopyrite to 10% is found along the margins of some
veins. Locally visible gold is noted in and along quartz vein
margins. Samples with the highest gold values come from the
siliceous layers.  Sampling results: One 1984 composite grab sample
assayed at 0.90 g Au/t over 0.5 m In 1986 a rock grab sample ran 80.
61 g/t Au and a chip sample had a cut grade of 15.52 g/t Au over 3.
26 m. As well 9 samples had assays over 10 g/t Au, 5 were between 3
& 10 g/t Au and 11 samples assayed between 0.5 and 3 g/t Au. 1987
sampling of the interbedded silicate iron formation yeilded assays
of 8.00 g/t Au over 5.15 m: 3.32 g/t Au over 4.7 m and 1.61 g/t Au
over 2.7 m. The 1988 drilling and sampling of the greywacke-
siliceous unit produced drill core samples of 0.95 g/t Au over 1.2
m: 1.91 g/t Au over 2.99 m and 5.72 g/t Au over 0.85 m.
The Komatik Lake Showing is in the SW section of the George Lake
area. The George Lake area lies within the northeastern portion of
middle greenschist.  In the George Lake area, iron formations
within Beechey Lake sedimentary rocks strike northwest. This 16 km
long and 2.5 km wide iron formation/sediment sequence has three
major oxide iron formation belts identified within it. These belts
are: the George Lake belt, the Fold Nose belt and the Lookout Hill
belt.  Komatik Lake is in the SW section of the George Lake area,
on the west side of the George Lake Belt, approximately 6.8 km from
the George Lake Camp (SW shore of George Lake). The Komatik Lake
area has had the following work done: prospecting, mapping,
sampling and in 1985 a Digham airborne geophysical survey was done
as part of the George Lake area. The airborne survey shows a 1.2 km
long shear related AEM conductor in the Komatik Lake area.
belts of the George Lake area as well as the main mineral
occurences and their locations.   The Komatic Lake showing is
within a NW trending subvertical greywacke and mudstone sequence
that is cut by NW trending intermediate composition porphyritic
dykes. The greywacke and mudstone are sheared subparallel to
bedding. A narrow gold and sulphide bearing (0.5 m wide) quartz
vein which has a strike length of approximately 50 m is within the
sheared mudstone unit.  Locally the quartz vein has ( by volume) up
to 10% arsenopyrite, 5% pyrite and 3% galena. Trace sulphides are
present in the dykes but are restricted to widely spaced
crosscutting quartz veins.  In 1987 a grab sample of 33.60 g/t Au
was assayed from a quartz vein with 10% arsenopyrite, 5% pyrite and
trace galena. A quartz vein sample with 3% pyrite, 3% galena and
trace arsenopyrite assayed 4.9 g/t Au and a quartz vein sample with
no sulphides assayed 0.69 g/t  Au.  In 1988  follow up sampling was
done. Of nine samples taken, all assayed less than or equal to 0.82
g Au/t.
The Mouse showing is in the SW section of the George Lake area. The
George Lake area lies within the northeastern portion of the
belt.  The Mouse showing is in the SW section of the George Lake
area, on the west side of the George Lake Belt, approximately 7.5
km from the George Lake Camp (SW shore of George Lake). The Mouse
sampling, ground geophysics and in 1985 a Digham airborne
geophysical survey was done as part of the George Lake area.
The Mouse showing is a NW striking sequence of mudstone and iron
formation that exists between two gabbroic dykes. The Mouse showing
is  a sulphide and gold bearing amphibole-chert-chlorite iron
formation that locally has up to 10% volume pyrite and trace to 5%
arsenopyrite.  Quartz veins crosscut the iron formation and
mudstone sequence. The iron formation has a strike length of
approximately 165 m.  One assay from 1984 gave a gold value of 33.
09 g/t over 2 m.  In 1985 a composite sample assayed at 2.5 g/t Au
over 1.2 m and a grab sample had a gold value off 2.5 g/t.
The Bullwinkle showing is in the SW section of the George Lake area.
Intrusive rocks of Hudsonian age and younger  diabase dykes
crosscut the older lithologies.  The George Lake Area is within the
belt.
The Bullwinkle Lake showing is in the SW section of the George Lake
area, within the Fold Nose belt, approximately 9 km from the George
Lake Camp (SW shore of George Lake). The Bullwinkle area has had
the following work done: prospecting, mapping, sampling, and in
1985 a Digham airborne geophysical survey was done as part of the
George Lake area.   Both silicate and oxide iron formations are
present within the Bullwinkle Lake showing.  In 1986 a rock chip
sample of oxide iron formation with arsenopyrite, pyrite and a
crosscutting quartz vein assayed at 6.51 g/t Au over 0.2 m.  Along
strike of this sample a composite grab sample yeilded an assay of 0.
82 g/t Au over 2 m.   A silicate iron formation 200 m SW of Rifle
Lake outcrops on the east side of a gabbro dyke and is undr 2 m
wide. A grab sample from this iron formation assayed at 6.0 g/t Au.
On the west side of the dyke (250 m SE) the silicate iron formation
has a strike length of approximately 10 m and is comprised of chert
and chloritic greywacke. A sample containing arsenopyrite and
pyrite assays at 2.81 g/t Au.  An oxide iron formation has trace
amounts pyrite and assays of grab rock samples range from 0.45 g/t
Au to 1.89 g/t Au.  A silicate iron formation to the NE of
Bullwinkle Lake parallels the SW edge of a large gabbroic dyke.
This iron formation has up to 50 volume percent arsenopyrite, 5%
pyrite and vein quartz. One assay gave a gold value of 19.89 g/t.
The Takrark Lake showing is in the SW section of the George Lake
area, within the Fold Nose belt, approximately 5.4 km from the
George Lake Camp (SW shore of George Lake). The Takrark Lake area
has had the following work done: prospecting, mapping, sampling,
and in 1985 a Digham airborne geophysical survey was done as part
of the George Lake area.   The Takrark Lake area gold bearing oxide
iron formation has discontinuous outcropppings that range from 7 to
20 m in width. Quartz veins crosscut the iron formation. The iron
formation contacts mudstone to the east and greywacke and a
gabbroic dyke to the west. The iron formation is a gold and
arsenopyrite-pyrite, chlorite magnetite chert iron formation that
has up to 50% coarse grained arsenopyrite and 2-10% pyrite. Visible
gold is associated with quartz veining as well as with arsenopyrite,
pyrite and chlorite.  In 1984 two samples 12 m apart along strike
yeilded assays of 16.63 g/t Au over 4m and 86.85 g/t Au over 0.3 m.
In 1986 a chip sample assayed at 40.36 g/t Au over 1.4 m (32.34/1.
4 m cut grade), 30 m to the SE a grab sample of arsenopyrite and
quartz vein assayed at 10.18 g/t Au.  The highest gold value from
1988 sampling was a grab sample with vein quartz, arsenopyrite and
pyrite. This sample assayed at 30.93 g/t Au.
The 4LBZ005 showing is in the SW section of the George Lake area
which  lies within the northeastern portion of the Archean Slave
Structural Province. This showing is located within the Lookout
Hill belt, approximately 10.8 km from the George Lake Camp (SW
shore of George Lake). The 4LBZ005 area has had the following work
done: prospecting, mapping, sampling, and in 1985 a Digham airborne
geophysical survey was done as part of the George Lake area.   One
sample was taken from the 4LBZ005 arsenopyrite-pyrite bearing
amphibole-chert-chlorite iron formation. This iron formation is
well banded and contains up to 5 volume percent coarse grained
arsenopyrite and 5% disseminated pyrite. Quartz veins are present
in the vicinity. This iron formation has an exposed strike length
of approximately 20 m and a gold bearing zone 0.8 m wide. One
sample was taken and assayed at 12.82 g Au/t over 0.8 m. in 1984.
The West Rapids showing lies within the northeastern portion of the
Archean Slave Structural Province. The principal underlying
consist mainly of volcanics and metasediments.  The Western Rapids
showing is in the Southern section of the George Lake area, along
strike of the Fold Nose belt, approximately 11.3 km from the George
Lake Camp (SW shore of George Lake). The Western Rapids area has
had reconnaissance sampling and, in 1985 a Digham airborne
geophysical survey was done as part of the George Lake area.   The
Western Rapids oxide iron formation is a small outcropping that is
cut by a 0.5 m wide quartz vein that has arsenopyrite, pyrite and
graphite along the margins. In 1983 a composite rock sample assayed
0.3 g/t Au across 4.0 m (Conkin et al, 1988). Sampling from 1988
yeilded assayes up to 28.18 g/t Au.
The Oar Lake showing is in the Southern section of the George Lake
The Oar Lake showing is in the southern section of the George Lake
area, along strike of the Lookout Hill belt, approximately 12.4 km
from the George Lake Camp (SW shore of George Lake). The Showing
outcrops at the NW end of Oar Lake. The Oar Lake area has had
reconnaissance sampling, mapping, trenching, drilling and, in 1985
a Digham airborne geophysical survey was done as part of the George
Lake area.   The Oar Lake gold bearing zone occurs in a pyrite
bearing iron formation that is interbedded with a chert-chlorite-
carbonate iron formation and mudstone sequence. The iron formation
contains crosscutting quartz veins, minor folds and faults. To the
south and east of the showing the Archean-Aphebian unconformity
outcrops.  In 1983 a composite grab sample of a arsenopyrite and
pyrite bearing felsenmeer boulder assayed at 27.91 g/t Au across 0.
5 m (Burlet et al, 1984). In 1984 a trench was excavated, exposing
a 1.32 m wide pyrite bearing iron formation with localized
arsenopyrite. An assay of 2.19 g/t Au over 1.32 m was recovered
from the trench. Approximately 180 m NW of the trench along strike
of the iron formation an assay of 10.05 g/t Au across 1 m was
recovered.  In 1985 the Oar Lake showing had airborne and ground
geophysical surveys  done as well as 168.86 m of drilling in two
diamond drill holes.
Ground magnetic anomalies coincide with surface exposures of oxide,
silicate and sulphidic iron formations at Oar Lake.  A VLF-EM
conductor is coincident  with the iron formation in the trenched
area.  The airborne magnetics, enhanced magnetics and VLF-EM
results indicate that the Oar Lake iron formation continues beneath
Oar Lake to the SE, but it is dextrally offset by approximately
110m by a NE trending fault.   Two drill holes totalling 168.86 m
were drilled. DDH 5B030 was drilled to test the down dip extension
of the previously trenched area. This DDH intersected the gold
bearing iron formation and assayed up to 4.39 g/t Au over 0.41 m
core length. DDH 5B031 was drilled to test the strike and down dip
extension of the gold bearing zone that assayed 10.05 across 1m g/t
Au. This DDH intersected the iron formation and an assay of 0.95 g/
t Au across 2.63 m core length was recovered.
The Shadow Pond showing is in the eastern section of the George
Lake area. The George Lake area lies within the northeastern
portion of the Archean Slave Structural Province. The region is
bordered by the Aphebian age Bear Structural Province to the west,
and the Rae Structural Province to the east. The principal
underlying supracrustal rocks belong to the Archean Yellowknife
Supergroup and consist mainly of volcanics and metasediments.
Archean intrusive and metamorphic rocks also underlie the region.
Early Proterozoic (Aphebian) clastic sedimentary and carbonate
sequences of the Goulburn Group unconformably overlie the Archean
rocks locally. Intrusive rocks of Hudsonian age and younger diabase
dykes crosscut the older lithologies.  The George Lake Area is
within the Back River region. The Yellowknife Supergroup in the
property area is divided informally into three major sequences.
The Back Group is the lowest sequence and is comprised of felsic to
Lake area, along strike of the Lookout Hill belt, approximately 3.4
km NE of the George Lake Camp (SW shore of George Lake). The Shadow
Pond area has had reconnaissance sampling, mapping at a 1:10,000
scale, and, in 1985 a Digham airborne geophysical survey was done
as part of the George Lake area.   The Shadow Pond silicate iron
formation is approximately 6 m wide and consists of interbedded
chloritic silicate iron formation, chert and chloritic greywacke.
Widely spaced crosscutting quartz veins are associated with all
anomalous gold values. Arsenopyrite and pyrite occur in zones (up
to 1 m wide) that parallel the margins of the quartz veins. In 1986
reconnaissance one grab sample yeilded an assay of 18.10 g/t Au and
a composite grab sample had an assay of 6.17 g/t Au over 6 m.
Samples collected between the quartz veins have little to no
visible sulphides and assayed less than 1.00 g/t Au.  An oxide iron
formation that has lenses of carbonate-magnetite-chert iron
formation outcrops approximately 180 m SE of Shadow Pond. The
carbonate rich portions of the iron formation are associated with
disseminated to finely layered pyrite beds. A composite grab sample
had an assay of 0.38 g/t Au over 3 m. In 1988 a grab sample from
this outcrop assayed at 1.03 g/t Au.
The Lookout Hill showing is in the eastern section of the George
Lake area, along strike of the Lookout Hill belt, approximately 2
km NE of the George Lake Camp (SW shore of George Lake). The
Lookout Hill area has had reconnaissance sampling, mapping,
drilling and, in 1985 a Digham airborne geophysical survey was done
as part of the George Lake area.   The Lookout Hill sediments are
comprised of a subvertical sequence of greywacke, siliceous
greywacke, mudstone, iron formation and a siliceous unit. These
sediments are tightly folded in a large syncline that plunges 38
degrees southeast and is offset by three steeply dipping faults.
The well banded iron formation consists of carbonate, amphibole,
magnetite, chlorite and chert. Along the east arm, and in
particular, the fold nose of the iron formation the carbonate
content is higher than in other sections of the George lake area.
The carbonate rich portions of the eastern arm of the iron
formation have massive to disseminated pyrite and pyritre nodules,
the fold nose has disseminated pyrite.  Approximately 330 m north
of the main fold nose a discontinuous siliceous unit that is
interbedded with greywacke and mudstone is exposed in felsenmeer.
This siliceous unit contains up to 15% pyrite and trace amounts
arsenopyrite. This unit is the northwest extension of the Shadow
Pond siliceous unit and sequence of the Rifle Lake interbedded
siliceous unit, iron formation and greywacke.
Reconnaissance prospecting and sampling was done at Lookout Hill in
1983 but all grab samples of the sulphidic and carbonate iron
formation assayed under 0.04 g/t Au. In 1984 this area was mapped
at a 1:10,000 scale and again prospected (Johnston et al, 1985).
In 1985 of nine samples assayed, only one assay was over 0.07 g/t
Au, that sample was taken from a thin pyrite bearing silicate iron
formation between Lookout Hill and the Slave occurrence. That
sample assayed at 0.17 g/t Au. From the 1985 airborne geophysical
survey, several AEM conductors to the southwest and at Lookout Hill
were noted.   1986 exploration included detailed prospecting, grid
surveying, sampling, geological mapping at a 1:2000 scale, ground
magnetometer, VLF-Em and HLEM surveying and drilling of one drill
hole to test the ground HLEM and VLF-EM conductors. The iron
formation in the drill core had up to 10 volume percent massive to
disseminated pyrite but drill core sampling in 1986 yeilded no
assays over 0.1 g/t Au.  In 1988 a siliceous unit north of the main
fold nose was sampled. Assays from rock grab samples ran up to 32.
61 g/t Au. Composite grab samples yeilded assays up to 1.99 g/t Au
over 1.5 m.
The Knight showing lies within the northeastern portion of the
consist mainly of volcanics and metasediments.  The Knight showing
is a single sample that was taken from an amphibole rich lean iron
formation that is less than 1 m wide and traceable for 750 m.
Sparse mineralization consists of up to 1% disseminated pyrrhotite.
The single sample from the iron formation had a gold value of 0.79
g/t Au, a second sample along the same horizon ran 0.17 g/t Au.
The U-1 showing lies within the northeastern portion of the Archean
Slave Structural Province. The region is bordered by the Aphebian
age Bear Structural Province to the west, and the Rae Structural
Hudsonian age and younger  diabase dykes crosscut the older
lithologies.  The U-1 showing is within the Aphebian rocks of the
Goulburn Group. These rocks, the Western River Formation, comprise
a thick succession of argillites, quartzites and dolomites that in
turn are overlain comformably by quartzites and conglomerates of
the Burnside River Formation.   Mineralization in the U-1 showing
consists of uranium, gold, and anomalous nickel and lead.
Assessment report 081178 notes that mineralization was discovered
in the Quartzite Member of the Western River Formation with the
predominant mineralized unit being a grey argillite-siltstone that
is carbonated locally. Mineralization was also found in altered
purple, seemingly porous quartzite. Massive dolomite and calcareous
sandstone in contact with the siltstone acts as a cap rock.
The argillite and siltstone are massive, fine grained, carbonated
and composed of sericite, chlorite and quartz. The siltstone
argillite interbeds are 6ft thick in places and weather whitish
orange. Fresh surfaces are black and veined with hematite. Frost
heaved radioactive boulders were traced for 1 3/4 miles NW from the
main mineralized area and stop abruptly where the Burnside
Quartzite begins. (See assessment report 081178 map 5 for the
location and proximity ofsample sites.)  Approximately 1 1/2 mi NW
from the main showing adjacent to the boulder train is a
mineralized outcrop in the quartzite member. The quartzite bed is
approximately 10ft thick locally and dips steeply.    Samples from
the showing were assayed for the following elements: U, Zn, Cu, Pb,
Ni, Ag, Au, and Th.   Significant results from the mineralized grey
argillite and siltstone range from 0.3% to 12.6% U3O8 and are as
follows:  Uranium: 4800, 3800, 3000, 8400, 12,6000, 7000 and 7000
ppm. Lead: 500, 575, 1070, 1050, 1120, 445 and 440 ppm. Nickel: 640,
380, 540, 1220, 1300, 720 and 620 ppm. Gold: 23,000, 16,000 and
3800 ppb.
The U-2 showing lies within the northeastern portion of the Archean
lithologies.  The U-2 showing is within the Aphebian rocks of the
the Burnside River Formation.   Mineralization in the U-2 showing
consists of uranium. Assessment report 081178 notes that
mineralization was discovered in the Western River Formation with
the predominant mineralized unit being a grey-green siltstone that
extends for approximately 400 ft. Associated with the siltstone is
a uniform, massive orange-brown quartzite. Calcareous quartzite was
found throughout the area.
In 1978 airborne reconnaissance was carried out over the U-2 area.
Radioactive showings were discovered and followed up in 1980 with
prospecting, mapping.  The results of prospecting within the U-2
showing area are noted on map 5 of assessment report 081178, they
are not listed or noted elsewhere. Samples range from 0.2 to 1.2 U
ppm. Also noted in the assessment report write up was that the
boulders and outcrops registered between 300 and 2000 cps
(Saphymostel SPPII).
The DEX showing lies within the northeastern portion of the Archean
lithologies.  The Yellowknife Supergroup in the property area is
sub-greenschist to upper amphibolite facies.
The  DEX showing area is predominantly steeply SW dipping greywacke
intercalated with black mudstone horizons that trend NW-SE. The
mudstone (argillite/siltstone) horizons have an average thickness
from 0.3 to 10 m wide (ranging from mm scale to 30 m). Greywackes
are fine grained and massive. Parallel to the regional bedding,
rare quartzite was mapped. The country rock is cut locally by NW-SE
trending diabase dykes.  The rock package has bedding planes
ranging from 135/80W to 160/75W and is slightly folded with the
fold axis trending at 240 degrees and plunging 75W. Faulting in
this area was in a similar direction. Quartz veining is common and
mainly parallel to bedding but also along joint planes. Quartz
veins to 15 m wide are noted and veins greater than 1 m are common.
Along several siliceous/quartz vein-rich zones, especially within
mudstone horizons shearing occurs parallel to subparallel to the
foliation. The shear zones have a range of 6-30 m wide. The quartz
is fine grained with banded horizons on the hanging wall margins
where the  shearing is most intense. A grid was emplaced over the
quartz flooded shear zones in 1990. The shear zones can be  traced
in the NW-SE direction for several hundred m and are truncated by
crosscutting (240 degree) faults.  The large quartz veins are often
gossanous with radiating amphibole needles and occasional chlorite
in fine grained clusters. Sulphide mineralization within the
siliceous shears is concentrated in the wall rock of the quartz
veins and consists of arsenopyrite > pyrite > pyrrhotite with
traces of chalcopyrite and bornite. Visible gold was also noted in
grab samples from quartz rich boulders.
The DEX showing area was initially reconnaissance prospected in
1989, then in 1990 it was more intensely mapped, sampled, a grid
was emplaced and five trenches excavated and sampled.  29 grab
samples were collected in 1989, 4 returned grades greater than 1 g/
t Au (1.74, 1.24, 1.55 and 1.31 g/t). 13 other samples had values
ranging between 135 and 925 ppb Au.  In 1990 123 samples were
collected in total, 14 had Au values greater than 1 g/t along 1.5
km NW-SE trending quartz flooded shear zones. 12 of the 14
anomalies were from grab or chip samples. They range between 1.04
and 7.09 g/t Au. 2 grab samples from angular quartz rich boulders
that flank a large shear zone had visible gold and had values of
105.2 and 60.2 g/t Au.
The Gaet 3 showing consists of a single sample from a minor
sulphide mineral occurrence within a banded iron formation. The NW
trending  interbedded  silicate/oxide banded iron formation occurs
within Beechey Lake Group turbiditic sediments of the Yellowknife
Supergroup. Reconnaissance mapping and prospecting resulted in
collecting one sample with a gold value of 0.55 g/t. This sample
had trace arsenopyrite and 1% pyrite.
The Trumpet showing lies within the northeastern portion of the
the older lithologies.  The Trumpet showing is within the
Yellowknife Supergroup which is divided informally into three major
sequences.  The Back Group is the lowest sequence and is comprised
of felsic to intermediate flows, tuffs and breccias. The Hackett
River Group overlies the Back and consists of  volcanic flows that
range from felsic to mafic, as well as tuffs and chemical sediments.
The uppermost sequence is the Beechey Lake Group, comprising
turbidite sediments, greywacke, mudstone and iron formation. Recent
mapping by the Geological Survey of Canada suggests that the
Hackett River and the Back volcanic belts, which are generally
spatially separate, may be coeval in their upper parts (Williamson
and Olson, 1990).  At least four periods of deformation have
affected the Yellowknife Supergroup. Metamorphic grade in the Back
River Region ranges from sub-greenschist to upper amphibolite
facies.  The Trumpet showing comprises sulphidic oxide and/or
silicate iron formations within  turbidites of the Beechey Lake
Group. A quartz diorite sill runs along strike adjacent to the NW
trending banded iron formations. These lithologies are cut by SW
trending mafic dykes.
Three gold mineralized satellite showings are associated with the
the Trumpet showing - the Oboe (Normin ID 076GNW0020), Piccalo
(Normin ID 076GNW0021) and Flute (Normin ID 076GNW0022). These
showings are located along strike of a silicate-oxide-sulphide
banded iron formation that trends NW for 1.7 km. Work in the area
consisted of reconnaissance mapping, prospecting, geochemical
sampling and a geophysical survey consisting of magnetometer and EM.
See Map 1 in  AR 083046 for relative locations.  Trumpet Showing:
Three styles of mineralization are reported over a distance of 40 m.
1) Semi-massive coarse grained arsenopyrite +/- pyrite with up to
80% arsenopyrite & 10% pyrite in chloritic sections. Grab samples
assayed up to 3.02 g/tonne gold. 2) Sulphide iron formations with
finely banded pyrite (5-50%) and arsenopyrite (up to 25%) and 3)
Bull quartz veins to 0.4 m wide with up to 5% pyrite within
metasediments. The veins are adjacent but not directly associated
with arsenopyrite and all vein samples had gold values <1 g/tonne.
Piccalo Showing  (Normin ID 076GNW0021):  The Piccalo showing
occurs in a 0.5 m wide, 100 m long amphibolitic (Silicate) iron
formation that has up to 3% arsenopyrite and minor pyrite in
chloritized sections. The sulphides are commonly associated with
crosscutting quartz veins. The highest grab sample assayed 0.72 g/
tonne gold.  Flute Showing (Normin ID 076GNW0022): Mineralization
is within 2 clusters of feldsenmeer boulders over a 45 m strike
adjacent to a 5-7 m quartz diorite sill. The boulders are up to 0.6
m wide and contain up to 75% euhedral arsenopyrite and 10% euhedral
pyrite in a chloritic matrix. The sulphide rich feldsenmeer appears
to be oriented with transverse quartz veins. The highest assay from
grab samples graded 5.90 g/tonne gold.
Oboe Showing ( Normin ID # 076GNW0020): Arsenopyrite and pyrite
mineralization is found over a  205 m strike length of oxide/
silicate iron formation that has a steep north trending dip. The
arsenopyrite occurs as disseminations in the banded sulphide as
narrow (<10 cm) veinlets and as semi massive clusters of crystals
(10-12%) in chloritized sections. Some of the sulphide occurrences
have sugary smokey quartz associated with them. The highest gold
value from a grab sample was 5.18 g/tonne.
This showing is part of the Trumpet showing. For further
information see 076GNW0019.  Oboe Showing ( Normin ID # 076GNW0020):
Arsenopyrite and pyrite mineralization is found over a  205 m
strike length of oxide/silicate iron formation that has a steep
north trending dip. The arsenopyrite occurs as disseminations in
the banded sulphide as narrow (<10 cm) veinlets and as semi massive
clusters of crystals (10-12%) in chloritized sections. Some of the
sulphide occurrences have sugary smokey quartz associated with them.
The highest gold value from a grab sample was 5.18 g/tonne.
information and references see 076GNW0019.  Piccalo Showing
(Normin ID 076GNW0021):  The Piccalo showing occurs in a 0.5 m wide,
100 m long amphibolitic (Silicate) iron formation that has up to
3% arsenopyrite and minor pyrite in chloritized sections. The
sulphides are commonly associated with crosscutting quartz veins.
The highest grab sample assayed 0.72 g/tonne gold.
information and references see 076GNW0019.  Flute Showing (Normin
ID 076GNW0022): Mineralization is within 2 clusters of feldsenmeer
boulders over a 45 m strike adjacent to a 5-7 m quartz diorite sill.
The boulders are up to 0.6 m wide and contain up to 75% euhedral
arsenopyrite and 10% euhedral pyrite in a chloritic matrix. The
sulphide rich feldsenmeer appears to be oriented with transverse
quartz veins. The highest assay from grab samples graded 5.90 g/
tonne gold.
The Buck showing lies within the northeastern portion of the
Archean) Slave Structural Province. The region is bordered by the
the older lithologies.  The Buck showing is within the Yellowknife
Supergroup which is divided informally into three major sequences.
sub-greenschist to upper amphibolite facies.  The Buck showing
comprises sulphidic oxide and/or silicate iron formations within
argillitic greywacke turbidites of the Beechey Lake Group. Feldspar
porphyry sills either run along strike or cut the N-NW trending
units of iron formation. Outcrop exposure ranges from 1- 40%.
The Buck Showing has 2 other  showings associated with it - the
Buck North Showing (Normin ID 076GNW0024), which is an extension of
the Buck showing  and the Chopin Showing (Normin ID 076GNW0025).
These zones are located along strike of a silicate-oxide-sulphide
banded iron formation that trends intermittantly NW for
approximately 2 km. See maps 1 & 2b in  AR 083055 for relative
locations.  Work done in the showing area has included
reconnaissance and detailed mapping, prospecting, geochemical
sampling (rock, drill core, till),  ground and airborne
magnetometer and EM geophysical survey, trenching, and diamond
drilling.   Within the Buck Showing  gold and sulphide
(arsenopyrite & pyrite) mineralization has been traced in drilling
and with surface geophysical surveys and mapping over a strike
length of approximately 600 m. Most of the heavy sulphide
mineralization is at or near feldspar porphyry sill contacts and is
hosted by either silicate or oxide iron formation. Grab and channel
samples have assayed up to 191.59 g/tonne Au. Trench samples have
gold values up to 17.83 g/t across 1.1 m. Drill core samples have
yielded gold values of up to 42.54 g/tonne across 1 m. Till samples
were were analyzed for gold and additional elements.  Buck North
(Normin ID 076GNW0024): The Buck North Showing is a northern
extension of the Buck Showing. The host iron formation is up to 40
m wide and towards the north tends to become increasingly oxide
rich. This showing has weakly developed, discontinuous zones of
pyrite and arsenopyrite within the iron formation. A rock grab
sample had a gold value of 1.85 g/tonne; all other grab or chip
samples were below 0.32 g/tonne Au.
Chopin Showing (Normin ID 076GNW0025): This showing is underlain by
the same unit of iron formation as the Buck and Buck North Showings.
The width of the Chopin oxide and silicate facies iron formation
ranges from 15 to 50 m and has been traced for approximately 125 m.
Gold mineralization is within sulphide rich zones with up to 10%
banded pyrite and pyrrhotite and up to 2% arsenopyrite. Sampling
returned values ranging from 1.37 to 6.55 g/tonne Au. One drill
hole tested the surface sampling and ground and airborne
geophysical targets. Sulphidic iron formation was intersected  and
confirmed surface sampling results. Gold values include 1.13 g/
tonne over 0.85 m, 1.20 g/tonne over 0.75 m and 2.69 g/tonne over 0.
30m.
This showing is part of the Buck showing. For further information
and references see 076GNW0023.  Buck North (Normin ID 076GNW0024):
The Buck North Showing is a northern extension of the Buck Showing.
The host iron formation is up to 40 m wide and towards the north
tends to become increasingly oxide rich. This showing has weakly
developed, discontinuous zones of pyrite and arsenopyrite within
the iron formation. A rock grab sample had a gold value of 1.85 g/
tonne; all other grab or chip samples were below 0.32 g/tonne Au.
and references see 076GNW0023.  Chopin Showing (Normin ID
076GNW0025): This showing is underlain by the same unit of iron
formation as the Buck and Buck North Showings. The width of the
Chopin oxide and silicate facies iron formation ranges from 15 to
50 m and has been traced for approximately 125 m. Gold
mineralization is within sulphide rich zones with up to 10% banded
pyrite and pyrrhotite and up to 2% arsenopyrite. Sampling returned
values ranging from 1.37 to 6.55 g/tonne Au. One drill hole tested
the surface sampling and ground and airborne geophysical targets.
Sulphidic iron formation was intersected  and confirmed surface
sampling results. Gold values include 1.13 g/tonne over 0.85 m, 1.
20 g/tonne over 0.75 m and 2.69 g/tonne over 0.30m.
Regional Geology:  The Lin showing lies within the northeastern
dykes crosscut the older lithologies.  The Lin showing is within
the Yellowknife Supergroup which is divided informally into three
amphibolite facies.  Property/Showing Geology:  The Lin showing
comprises sulphidic siliceous iron formations within greywacke
turbidites of the Beechey Lake Group. Mineralization occurs within
siliceous, arsenopyrite and pyrite bearing float over an
approximately 500 m strike which may be altered from two 1-2 m
thick silicate facies iron formations which are 25-30 m apart.
Exploration  done on the showing includes reconnaissance mapping
and sampling, grid establishment, detailed mapping and sampling at
a 1:1000 scale and a ground magnetic survey.  Initial grab samples
assayed up to 5.38 g/tonne Au, follow up channel samples yeilded
values up to 2.13 g/tonne across 0.75 m.
The Mozart showing has been subjected to reconnaissance mapping,
prospecting and sampling. This showing is located within an
extensive boulder field. The host for mineralization is a
porphyroblastic knotted schist and a porphyroblastic phyllitic
schist. Mineralization was traced along a 250 m strike length
(approximate) and consists of arsenopyrite to 9% and pyrite to 3%
within strongly silicified and quartz veined schists. Grab and
channel samples were anomalous, the highest grab sample had a gold
value of 6.62 g/tonne, the best channel samples gave results of 3.
19 g/t across 0.63 m and 1.03 g/t across 0.85 m.
The Bach showing lies within the northeastern portion of the
the older lithologies.  This showing is within the Yellowknife
Supergroup. Metamorphic grade ranges from sub-greenschist to upper
amphibolite facies.  The showing comprises oxide and/or silicate
iron formations within massive greywacke turbidites of the Beechey
Lake Group. Exposed strike length of this folded, 3 m wide iron
formation is approximately 500 m.
The iron formation of the Bach Showing was first noted in 1990 when
a grab sample taken during prospecting returned a gold value of 7.
51 g/tonne. Subsequent reconnaissance and target specific mapping
and geochemical grab and channel  sampling was done as follow up
work as was grid emplacement and a ground magnetic survey. The
magnetic survey identified a 50-100 m wide magnetic anomaly
interpretted to be an underlying iron formation.   Of 5 grab
samples taken, 1 had a gold value of 3.81 g/tonne. All other
samples had assays with gold values less than or equal to 0.1 g/
tonne. Of 8 channel samples, the three best were: 1.78 g/t across 0.
65, 2.95 g/t across 0.70 m and 1.17 g/t across 0.9 m. The remaining
samples had gold values below 0.82 g/t.
The Lin1 showing area has been subjected to reconnaissance mapping,
prospecting and sampling. The host for mineralization was a
slightly silicified greywacke with 1-3% pyrite. This showing is
from a single reconnaissance sample that is located on map 3a of AR
082994. It is noted that this sample is from previous
reconnaissance work.
The Lin 2 showing consists of a single reconnaissance sample of a
rusty weathering pyritic mafic sill. This sample had a gold value
of 0.58 g/tonne Au.
The WL1 showing lies within the northeastern portion of the Archean
lithologies.  The WL1 showing is within the Yellowknife Supergroup
which is divided informally into three major sequences.  The Back
amphibolite facies.  The WL1 showing comprises an oxide magnetite-
chert iron formation that strikes NNW through mudstones and minor
interbedded greywacke turbidites of the Beechey Lake Group. A
sulphide facies zone within the iron formation has an exposed
strike length of 10 m and a width of 2.87 m in a trench.
The WL1 Showing has been subjected to prospecting, reconnaissance
mapping, geochemical sampling and mapping on a 1:1000 scale, ground
magnetometer and VLF-EM surveys, rock trenching and rock chip
sampling.  The original reconnaissance geochemical sampling
produced gold values of 1.51 and 4.75 g/t. Follow up rock chip
sampling  from 8 samples across a trench produced gold values
ranging from 0.025 g/t to 3.0 g/t across 0.86 m. The ground
magnetometer and VLF-EM surveys delineated the iron formation and
the sulphide bearing zones within the iron formation.
This showing consists of 2 reconnaissance samples taken from
Yellowknife Supergroup  Beechey Lake  sediments. Sample 51621 is a
felsenmeer grab sample that had 1% arsenopyrite and 2-3% pyrite.
This sample had a gold value of 0.82 g/tonne. Sample 51622 was a
rock grab sample with 3-4% pyrite.  This sample had a gold value of
0.58 g/tonne.
This showing consists of a single reconnaissance sample comprised
of pyrite and arsenopyrite within a quartz vein. This sample had a
gold value of 0.51 g/tonne.
This showing is a single reconnaissance sample that had a gold
value of 0.51 g/tonne. No further information is available.
The DOX 0759 showing lies within the northeastern portion of the
Archean Slave Structural Province.  The principal underlying
consist mainly of volcanics and metasediments. The Dox 0759 showing
is from a band of interbanded pyritic meta-chert and amphibolite
which returned an assay of 0.62 oz/ton Au. The map accompanying
assessment report 061344 places this sample within a quartz
monzonite but the summary states that the sample is from a 0.5 by 4
mile belt that contains pyritic chert, graphitic-pyritic schist,
and amphibolite.
The Burnside area lies within the northeastern portion of the
Archean  Slave Structural Province. The region is bordered by the
Intrusive rocks of Hudsonian age  and younger diabase dykes
crosscut the older lithologies.  The Burnside Area is within the
sub-greenschist to upper amphibolite facies. In the Burnside area
the general metamorphic grade is middle greenschist.
The Burnside area is underlain by greywacke-argillite turbidite
sequences of the Beechey Lake Group which can be subdivided into
greywacke dominated (greater than 70% of the rock) and argillite
dominated units. Generally these sedimentary rocks have a NW strike
and dip from 50 to 80 degrees to the southwest. Regionally, the
beds are folded into large scale isoclinal folds about NW trending
axis.Crumpling of argilliceous beds is evidenced of a second phase
of folding about SW plunging fold axis. These folds are broken at
the hinge by steep angle faults trending NW. Displacement across
the faults is up to 400 m.  Arsenopyrite bearing argillite units
that are cut by crosscutting and conformable quartz veins host the
gold mineralization in the Burnside area. Within the argillite
units, gold mineralization is intimately associated with
arsenopyrite, pyrite, pyrrhotite and rare chalcopyrite which occur
both as disseminations and as medium to coarse grained aggregates
at the margins of conformable and crosscutting veins. Gold occurs
in native form; however, the close association of gold with
arsenopyrite implies that gold may also occur with this type of
sulphide. Disseminated sulphides, particularly arsenopyrite, are
preferentially concentrated in amounts to 20% in 0.5 to 2 cm
siliceous bands or wisp-like laminea (sic) conformable to the
bedding. Quartz veins, like the sulphides, are strata bound to
argillite dominated strata. Two forms of quartz veins are present,
an early phase of grey quartz occurring as lensoidal or rod-shaped
veins conformable to bedding and later crosscutting white to light
grey quartz veins. The earlier quartz veins often form rod-like
bodies within the cores of the minor phase two folds and are of
variable thickness. In the cores of folds these veins were observed
to be up to 50 cm thick. Where native gold was seen, it was in
these stage 1 veins (McClintock J.A.,1987).
South and west of Del Lake (See map 5/7 from assessment report
082070 for location of the area of mineralization and grids)
several distinct sulphide bearing and quartz veined argillite units
occur within a NW trending zone that is up to 400 m wide and has a
strike length of 3.6 km. Individual auriferous units are continuous
for up to 1 km along strike before pinching out into greywacke
units. Higher gold grade values are restricted to argillite units
that are deformed by phase 2 minor folds and have quartz and
arsenopyrite concentrations of 2-3%. These units are restricted to
200 m or less strike lengths.  In 1985, exploration consisted of
reconnaissance prospecting, 1:2000 scale geological mapping, total
field and vertical magnetic gradient surveys, and dip angle VLF
surveys. Gold assays of up to 60 g/t were obtained from grab
samples of quartz arsenopyrite veins in argillite. Grids were set
up over the most intensely mineralized zones. On the H-1 Grid a
total of 69 samples were collected and assayed for gold. Of these
samples, 1 assayed at 67.4 g/t, 2 were in the range between 25-30 g/
t, 1 assayed between  20-25 g/t, 1 was in the 10-15 g/t range, 5
ranged between 5-10 g/t, 23 were in the 1-5 g/t range, 27 assayed
between 1 and 5 g/t and 9 samples assayed less than 0.1 g/t Au. The
H-2 grid had a total of 20 samples assayed for gold.  Of these, 1
was in the range from 15-20 g/t, 1 ran between 10-15 g/t, 5 were in
the 5-10 g/t range, 11 in the 1-5 g/t range and 2 assayed between 0.
1 and 1.0 g/t Au.  In 1986 further work included reconnaissance
mapping and sampling, detailed mapping at a 1:1000 scale, trenching,
chip and channel sampling and in two areas, diamond drilling.
The two areas with consistent high gold values (over 1.0 g/t) are
the Beechey Zone (located on the west side of the H-2 grid) and the
Phoenix Zone (located at the south end of the H-2 grid). These two
zones were drilled and the drilling results showed gold content
decreased with depth. See Plate 1 from assessment report 082570 for
the locations.   Results from the Beechey Zone showed a strike
length of 110 m with gold grades up to 9.1 g/t Au over 9 meters.
Nine holes were drilled for a total of 537 m to further test the
mineralization . Mineralization was intersected that was similar to
that at surface but the gold grades were much lower. The highest
interval recovered was 5.4 g/t Au across 1 m core length.  The
Phoenix Zone had two holes drilled to a total of 73 m, these
results were also low grade with the highest intersection assaying
at 5.5 g/t Au across 1 m core length.
The Skarn showing area lies within the northeastern portion of the
by the Aphebian age (>1.9 Ga) Bear Structural Province to the west,
rocks locally. Intrusive rocks of Hudsonian age (1.8 Ga) and
younger (1.2 Ga) diabase dykes crosscut the older lithologies.  The
Skarn showing area is within the Back River region. The Yellowknife
amphibolite facies. In the Skarn showing area the general
metamorphic grade is middle
greenschist
Exploration in the Skarn showing area took place in 1986 with
reconnaissance mapping at a scale of 1:10,000 and prospecting. The
actinolite and actinolite-sulphide Skarn showing developed along
the contact of a granite plug with greywacke and argillite. The
plug measures 300 m by 80 m and is a leucocratic, hypidomorphic
granular biotite-hornblende granodiorite (Plate 2). The skarn zone
is up to 10 m wide and divisible into an actinolite and sulphide-
actinolite skarn. The actinolite skarn is comprised of massive
actinolite with lesser amounts of plagioclase and minor calcite.
The sulphide skarn, for the most part, contains up to 5%
arsenopyrie with lesser quantities of pyrrhotite and  pyrite.
Samples collected from the sulphide skarn contained between 0.01
and 0.16 g/t gold. Three pod-like bodies of massive sulphide occur
within the sulphide skarn. The largest occurs at the southern tip
of the intrusive and measures 4 m by 1 m. This sulphide pod is
composed of chalcopyrite, pyrite, pyrrhotite, arsenopyrite and
nicolite. Two grab samples of the sulphides assayed 7.25 and 2.24 g/
t gold. The other two sulphide pods are mainly arsenopyrite and
pyrrhotite. Samples from these sulphides assayed 0.14 g/t gold over
2 m, 0.12 g/t over 2 m, and 0.01 g/t over 2 m (McClintock, J.,1987).
The IRA showing lies within the northeastern portion of the Archean
(>2.5 Ga) Slave Structural Province. The region is bordered by the
Aphebian age (>1.9 Ga) Bear Structural Province to the west, and
the Rae Structural Province to the east. The principal underlying
Intrusive rocks of Hudsonian age (1.8 Ga) and younger (1.2 Ga)
diabase dykes crosscut the older lithologies.  The Yellowknife
amphibolite facies.
The IRA showing is within a small portion of a large granodioritic
intrusion (100 sq. km) that intruded the underlying Yellowknife
Supergroup turbidites and  minor volcaniclastic rocks. A number of
large mineralized quartz veins occur near the  intrusive contact. A
single major quartz vein is the primary focus of the IRA showing.
The main mineralization of the IRA showing is within a single vein
structure that is 10-20 m wide and traceable for a strike length of
approximately 1300m. The vein has been offset by at least two
faults which have a 100 m southward displacement. Movement of the
faults has been interpretted as near vertical.  Bubar, 1983,
interprets the east-west structure hosting the mineralized quartz
vein as an early joint plane as there is no evidence of offset
where the vein and contact meet.  Mineralization of the vein
material consists of white massive to sugary quartz with a variable
sulphide content (up to 50%). The most abundant sulphide mineral is
chalcopyrite (up to 75% of total sulphide content)followed by
pyrite, pyrrhotite and molybdenite.
The showing area has poor exposure with few outcroppings of the
mineralized quartz vein but it is well defined geophysically as a
continuous conductive zone. The sulphide rich portion of the vein
appears to be on the the hanging wall side (south side) of the vein.
Work conducted on the IRA showing includes mapping at a 1:2000
scale, HLEM and VLF surveys, bedrock trenching and grid
construction. The detailed geology map from assessment report
081682 shows the detailed geology and the placement of the grid.
Eight grab samples from the eastern portion of the of the vein
structure (grid line 0+00 to 6+00 averaged 4.87% Cu, 52.8 g/t Ag, 2.
1 g/t Au and 0.11% MoS2. EM surveys over this area identified a
strong conductor coincident with the mineralized frost heave
continuous over 500 ft. and with an estimated width of 10-20 m.
Two trenches were excavated, in the better of the two, three chip
samples assayed 2.466% Cu, 23.03 g/t Ag, 0.46 g/t Au and 0.146 MoS2
over 7 m or 1.954% Cu, 19.7 g/t Ag, 0.41 g/t Au and 0.146% MoS2
over the full 12.08 m trenched. The EM survey indicated that the
core of the conductor is situated coincident with an overburden
covered depression to the south of the trench which Bubar (1983)
suggests that the massive mineralization was not exposed in the
trenches.
The Beech 1 showing lies within the northeastern portion of the
consist mainly of volcanics and metasediments.   Reconnaissance
mapping and prospecting of the area around the  Beech 1 showing
took place in 1988 (no report) and 1990, concentrating on a N - S
trending metavolcanic unit that is approximately 400 m wide. The
Beech 1 showing is within a quartz vein swarm 50-100m wide and
approximately 700 m long, individual veins have an average width of
0.5 - 1 m with individual veins up to 2 m wide. The quartz veins
contain minor amounts of pyrite, pyrrhotite, chalcopyrite, galena
and native copper. The metavolcanic wallrocks are generally sheared
and gossanous and contain 10-15% pyrite and pyrrhotite locally.  Of
13 grab samples taken in 1990 of mineralized quartz vein material
the best value was 5.66 g/t Au. Two other samples assayed 2.91 and
5.55 g/t Au The other samples were less than 1 g/t Au. A 1988
sample assayed at 7.30 g/t Au but when it was resampled in 1990 it
assayed 0.07 g/t Au suggesting that  gold distribution may be
erratic within the quartz veins.  In 1993 exploration work was done
over the general claim  area to determine the potential for
locating diamond occurrences.  A fence of till, soil and 3 rock
(for ICP) samples were collected to sample for indicator minerals.
One spinel of interest was recovered by sampling and was
interpretted to be from a lamproite rather than a kimberlite.
The Beech  showing lies within the northeastern portion of the
consist mainly of volcanics and metasediments.  Reconnaissance
mapping and prospecting of the area around Beech showing took place
in 1988 (no report submitted) and 1990 and concentrated on a NS
Beech showing consists of three localities within the  hinge area
of a possible fold structure that have gold bearing quartz veins.
A grab sample from a 10 cm wide quartz vein which contained 5%
pyrrhotite, 1% chalcopyrite, 1% pyrite and traces of native copper
assayed at 67.71 g/t Au. Other assay values from the area were 3.77
g/t, 1.20 g/t, 0.99 g/t and 0.58 g/t Au. Generally the area of the
showing is poorly exposed.
The Casey Lake  showing lies within the northeastern portion of the
consist mainly of volcanics and metasediments.  The Casey Lake area
is underlain by Yellowknife Supergroup clastic metasediments which
are cut off to the south by a granitic pluton. A thin, NW striking,
steeply dipping band of intermediate to mafic volcanic rocks with
associated iron formation occur within the sedimentary sequence.
The iron formation is mainly  silicate -  sulphide facies with
locally up to 15% pyrite +/- pyrrhotite. The iron formation (5-20 m
wide) was sampled at 100-150 m intervals along the exposed strike
length of  approximately 8 km. Rock and soil samples were analysed
for Cu, Pb, Zn, Ag, As and Au. The Casey Lake showing consists of
two samples that had assays above the cutoff for zinc (3100 & 3800
ppm), no other samples wereabove the cut off grade .
consist mainly of volcanics and metasediments.  At the GM7
occurrence, minor felsic volcanics/dacite are found as thin
horizons with the intermediate volcanics. The metavolcanics were
mapped as a series of fault bounded lenses within a granite
intrusion and may be distal correlates of the Back River volcanic
complex (Assessment report 081656).   Sampling of the area included
rock and soil samples assayed for Cu, Pb, Zn, Ag, As, and Au. The
GM7 showing consists of one rock sample from pyritic (10% ) dacite
that assayed at 3300 ppm Zn.
The Musk massive sulphide occurrences are located in the Hackett
River greenstone belt of the Slave structural province. They occur
near the transition between a dominantly mafic sequence and an
overlying, dominantly sedimentary sequence. This stratigraphic
position is generally occupied by a carbonate-rich, felsic
pyroclastic-tuff sequence which is well-developed.   The immediate
area of the Musk showing is underlain by a sequence of volcanic
rocks capped by chemical sediment. The deposit footwall comprises a
complexely interbedded sequence of rhyolite tuffs, lapilli tuffs
and crystal tuffs together with minor agglomerate and thin
rhyolitic flows. Massive sulphides occur near the top of a well-
foliated, recrystallized rhyolitic tuff and are manifested in a
number of small gossans sporadically developed over a 700 metre
strike length. Immediately overlying this mineralized unit are
massive pillowed basalt flows characterized by carbonate amygdules
and discontinuous zones of carbonate-cemented breccia. This unit is
overlain by a series of andesitic tuffs and flows which is in turn
overlain by a package of interbedded rhyolitic, rhyodacitic and
dacitic tuffs and agglomerates, all of which are carbonate-rich.
This final sequence is capped by cherty, carbonate-rich tuffites.
Diamond drilling has intersected two zones of
base metal enriched massive sulphides. The upper zone comprises
disseminated and poorly bedded to veined sphalerite, galena and
chalcopyrite with lesser pyrite and pyrrhotite, in an altered
felsic lapilli tuff.
The lower sulphide horizon consists of massive sphalerite and
pyrite together with lesser pyrrhotite and galena. Chalcopyrite is
most typically found as stringer veins and disseminations in the
basal portions of the mineralized zones although it is present in
minor amounts throughout. Rough banding can be seen in some areas
and a gradation from a Zn-rich top to Cu-rich base is apparent in
most drill intersections.  Footwall alteration consisting of
chlorite, biotite, talc, sericite, garnet and minor anthophyllite
is variably developed below the mineralized horizon, which itself
is strongly silicified and is characterized by moderate chlorite,
biotite and carbonate alteration.  Work has been done on the Musk
showing area since 1974 and includes: an airborne survey which
identified a two line anomaly, this was followed up with geological
mapping and geophysical surveys including magnetometer, VLF-EM,
VLEM which identified sulphide mineralization in outcrop. Another
pass of geophysical surveys were done later on which included
gravity fluxgate magnetometer, HLEM, VLEM and VLF-EM as well as
geological mapping and diamond drilling (13 ddh totalling 1395 m).
A conductor was identified and drilling intersected high grade
massive sulphides. A follow up program of diamond drilling was done
(23 ddh totalling 2570 m) which outlined a geological inventory of
387,000 tons grading 1.2% Cu, 1.39% Pb, 10.38% Zn, 10.87 oz/ton Ag
and 0.049 oz/ton Au. Note: this geological inventory is based on a
total of 36  diamond drill holes.  The latest (1994) work done on
the showing was a DeepEM survey. AR
083324
Reconnaissance work was done over the HUNT Group Claims which
included mapping, sampling and ground geophysical work including
magnetometer and VLF-EM. No samples analysed had assay values above
the database cutoff. The location of showing is the approximate
centre of the Claim Group.
The Fidler Lake area lies within the northeastern portion of the
the older lithologies.  The Yellowknife Supergroup in the property
Only 10% of the showing area is underlain by outcrop, the majority
of which are Beechey Lake Group sediments (NW striking, steeply
dipping) consisting of thin bedded to massive greywacke and
interbedded mudstones. Locally, interbedded magnetite-amphibole-
chlorite-chert iron formations exist within the greywackes in
narrow belts. Faults and shear zones trending W-NW cut through the
Beechey Lake Group rocks.  Gold is associated with sulphide
minerals within narrow discontinuous chlorite rich zones that exist
adjacent to white quartz veins that cut the iron formation and
greywacke. Typically, the quartz veins are concentrated within or
near iron formation +/- greywacke, are oriented either
perpendicular or parallel to the bedding of the sediments, range in
width from 1 to 50 cm, and have strike lengths to 5 m. The chlorite
rich sulphide bearing zones range from 0.1 to 3 m wide.  The Fidler
showing has been subjected to periodic exploration since 1946,
including mapping, prospecting, geochemical sampling, establishing
a grid and ground magnetometer surveying.  Assays from
reconnaissance sampling gave results of 0.63 oz/T Au, 0.26 oz/T Au
and 0.02 oz/T Au.  Grid sampling in conjunction with mapping gave
values of 4.3 g/t Au over 3 m (chip , 6.24 g/t Au, 5.52 g/t, 1.06 g/
t and 0.965 g/t Au from grab samples.
The Ack showing  lies within the northeastern portion of the
the older lithologies.  The Yellowknife Supergroup is divided
coeval in their upper parts.  At least four periods of deformation
have affected the Yellowknife Supergroup. Metamorphic grade ranges
from sub-greenschist to upper amphibolite facies.
The Ack Showing is underlain by argilliceous greywacke interbedded
with silicate facies iron formation of the Beechey Lake Group and
the volumetrically less important mafic tuffs, felsic volcanic
flows and mudstones of the Ignerit formation (upper formation of
the Hackett River belt). Two bands of mineralized iron formation
have been identified within the showing area and have been called
historically either Showing #1 (or Main or Western) & #2 (or
Eastern). See figure 2 from assessment report 082964 for location.
The Ack showing has been subjected to intermittant exploration
since 1964. Work done on the area includes mapping - both
reconnaissance and detailed, geophysical surveys - magnetometer and
self potential, magnetic total field and VLF-EM, geochemical
sampling, ICP, petrographic studies and diamond drilling.
Geochemical sampling in assessment report 017134 listed grab sample
gold values as ranging from 0.43 to 0.64 oz/ton (Showing 1) and 0.
61 to 0.84 oz/ton (Showing 2).  Eight diamond drill holes were
drilled in the Ack Showing area in 1964 for a total footage of 1485
feet. No assays had gold values above the data base cutoff.
Sampling during 1982 yeilded the following gold values: 17,143 ppb,
34,286 ppb and 27,249 ppb Au.  In 1988 & 90 work done in the
showing area included further prospecting, mapping, geochemistry
(rock and soil sampling for Au and ICP) and geophysics (mag & VLF-
EM). The geophysical work done suggests the presence of extensive
silicate iron formation and oxide iron formation under overburden.
In total 78 rock samples and 2 soil samples were collected. 16
samples had gold values ranging between 660 ppb and 40,800 ppb. 15
of these 16 samples ran above 1500 ppb Au. The 5 highest assay
values were: 40,8000, 29,900, 23,090, 17,300, and 15,300 ppb Au.
The Needle Lake area lies within the northeastern portion of the
the older lithologies.  The Needle Lake Area is within the Back
sub-greenschist to upper amphibolite facies. In the Needle Lake
area the general metamorphic grade is upper greenschist but within
300 m of the Regan Intrusive Suite plutons the grade increases to
lower amphibolite grade and are increasingly deformed.
Unmetamorphosed felsic dykes are common in the Needle Lake area and
appear to be spatially associated with the Regan Suite rocks.
Three periods of iron formation deposition have been identified
within the Back and Beechey Lake Groups (Chandler et al, 1992). In
the property area, iron formations are believed to be equivalent
stratigraphically to the uppermost iron formations in the Beechey
Lake Group.  The Beechey Lake Group in the Back River region are
isoclinally folded greywackes, siliceous greywackes and mudstones
that are interbedded with iron formation and are steeply dipping.
The iron formation consists mainly of magnetite and chert and is of
the oxide variety. Subordinate amounts of silicate iron formation
are also present (Williamson and Olson,1990).   In the Needle Lake
area the steeply dipping Yellowknife Supergroup rocks are folded
into a regional scale anticlinorium that has a SE plunge. The
Beechey Lake Group sediments, which include the iron formations,
occur within a E-SE striking belt. Where the Regan Intrusive Suite
rocks intruded, the trend of the Beechey Lake sediments is parallel
to the trend of the plutons.  Both oxide and silicate iron
formations occur within a sequence of interbedded greywacke and
mudstone but there is poor exposure as Quaternary glacial sand,
gravel and boulders cover approximately 90% of the Archean
Yellowknife Supergroup rocks in the Needle Lake area.  The well
banded oxide iron formation contains magnetite, chert, amphibole
and locally garnet. The poorly banded silicate iron formation
contains amphibole, chert, chlorite and garnet. Locally, both the
oxide and silicate iron formations contain sulphides which are
associated with white quartz veins that crosscut greywacke and
mudstone. The width of the iron formations range from 1 to 30 m,
the strike length is approximately 1.2 km.
Ground geophysical data indicates that the iron formations are
complexly folded. The pattern exhibited by the magnetic contours at
Needle Lake area indicates that a belt of iron formation has been
openly folded into a large S shape. The length of this S shaped
fold from Pumpkin Lake to Needle Lake, Needle Lake to Dog Lake, and
Dog Lake to Scissors Lake is about 8 km.  A north-striking,
easterly dipping, strong intensity positive magnetic anomaly
indicates that the iron formations in the central portion of this S
shaped fold are tight to isoclinally folded. The pattern exhibited
by these positive magnetic anomalies indicate a fold closure exists
at or near the north end of Needle lake and at or south of Dog Lake
Williamson & Olson, 1990. See Dwgs. 0605.N-2 from assessment
report 082980 for the locations mentioned.  Gold bearing sulphide
zones in the iron formations at Needle Lake are associated with
quartz veins or zones of silicification. The most common sulphides
are pyrite and pyrrhotite. Less common is arsenopyrite.
Arsenopyrite occurs as fine- to medium-grained, disseminated
acicular crystals and as massive bands that are invariably at or
near the margins of quartz veins or quartz-rich zones within the
iron formation. In general, gold occurrences within the Needle Grid
comprise arsenopyrite-bearing zones associated with quartz veins in
iron formation. However, in places, rock samples that were
collected from pyrite-bearing quartz veins in iron formation with
no arsenopyrite, assay greater than 10.0 grams gold per tonne (g/t
Au). Williamson & Olson,
1990
Exploration, including reconnaissance prospecting and sampling in
the Needle Lake area has taken place since 1983 (Johnston et al,
1985). In 1985 detailed exploration was done within the Needle Lake
area including rock chip sampling, trenching, overburden sampling
and geological mapping at a scale of 1:25. The 1985 season also
included further reconnaissance prospecting, sampling and mapping
at a 1:10,000 scale.  The 1985 rock samples were collected from
along the northwest and southeast shoreline of Needle Lake in two
belts of iron formation and from a third belt of iron formation
southwest of Scissor Lake.  Rock chip samples which were collected
from sulphide bearing iron formation in trench 85-7 assay up to 11.
66 grams gold per tonne (g/t Au) across 1.5 m (Dwg. 5602-73). Rock
chip and rock grab samples which were collected during
reconnaissance prospecting from sulphide bearing zones within iron
formation, assay up to 43.65 g/t Au across 0.33 m and up to 28.97 g/
t Au respectively. Rock chip and rock grab samples which were
collected from sulphide bearing quartz veins hosted by greywacke or
schist derived from greywacke, assay up to 12.38 g/t Au. Such gold
bearing quartz veins are usually less than 0.25 m wide and have a
strike length of less than 10 m. They are, as well, typically near
gold bearing iron formation. Rock chip and rock grab samples that
were collected from sulphide bearing zones within greywacke,
mudstone or schist derived from greywacke that lack quartz veins,
assay 0.10 g/t Au or less (Johnston et al,1985).
1986 exploration included a ground magnetometer & VLF-EM survey,
prospecting, rock sampling and geological mapping at a scale of 1:
2000 and 1:50.  Twelve geographic locals had gold occurrences where
samples assayed greater than 3.00 g/t Au. Three rock chip and 27
rock grab or composite rock grab samples were collected at the
Needle Lake area. Gold assays range from less than 0.07 to 148.73 g/
t Au (Dwgs. 6601-207 and 6601-208). Six rock samples assay greater
than 10.00 g/t Au, eight rock samples assay between 3.00 and 10.00
g/t Au, and five samples assays less than 0.5 g/t Au. Dufresne &
Johnston, 1986.   Ground exploration was not performed between 1987
and 1989 in the Needle Lake area.  In 1988 & 1989 Aerodat Ltd.
performed airborne geophysical surveys in the Needle Lake area.  In
1990 the area was subjected to grid surveying, prospecting, rock
sampling, ground magnetometer and VLF-EM surveying, geological
mapping at a 1:2,000 and 1:5000 scale and diamond drilling.  A
total of 24 composite rock grab samples, 204 grab samples and 91
drill core samples were assayed. 1,287.47 m of core was drilled in
13 holes, 11 holes at the Needle target and 2 at the Feline target.
All 13 diamond drill holes intersected at least one unit of oxide
iron formation. Two holes had no sulphides, quartz veins or
associated alteration and were not sampled, five holes contained
narrow gold bearing sulphidic zones, two holes had visible gold.
One drillhole intersected a 4.93 m wide sulphidic zone with low
gold content, and three drill holes intersected gold bearing zones
that had a gold grade times true width product greater than 20
grams times metres.
The Moth Valley area lies within the northeastern portion of the
the older lithologies.  The Moth Valley area is within the Back
are also present (Williamson and Olson,1990).  In the Moth Valley
area oxide iron formations with thin interbeds of silicate iron
formation occur within a sequence of interbedded greywacke and
mudstonet. Oxide iron formation is generally well banded and
contains magnetite and chert, with lesser amounts of chlorite,
amphibole and garnet. Silicate iron formation is poorly banded and
contains chlorite, amphibole, chert and garnet. Both types of iron
formation contain sulphides. In addition, they both contain thick
interbeds of greywacke or mudstone or both. In fold noses, the iron
formation and interbedded greywacke and mudstone form a unit that
is up to 100 m thick. Individual beds of iron formation within
these fold noses are up to 30 m thick. Williamson & Olson, 1990.
The sequence of Beechey Lake Group sedimentary rocks in the Moth
Valley area is approximately 4 km in length and ranges from 0.6 to
1.5 km in width between Archean granitic plutons which occur to the
north and south. West trending shear zones exist within the
sedimentary sequence, subparallel to the stratigraphy. Several of
the shears are silicified.  No Archean dykes or unmetamorphosed
Helikian gabbroic dykes are present in the Moth Valley area.
Three separate gold occurrences are noted in the Moth Valley area
(Blaster, Moth and Valley). The Valley and Moth occurrences exist
along the same linear, siliceous shear zone. The Blaster occurrence
is 250 m along strike of the last mapped portion of the siliceous
shear zone. The siliceous shear zone exists  subparallel and along
the south limb of an east closing fold defined by oxide iron
formation and has been traced in outcrop for approximately 1.5 km
along strike. Within this shear zone, individual shears range from
0.1 to 1 m in width. Where two or more parallel shears exist they
are usually 10 to 20 m apart. Iron formation or greywacke or both
host the siliceous shear zone.   Gold occurrences in the Moth
Valley are associated with sulphide bearing portions of iron
formation. The siliceous shear zone of the Moth Valley area
contains an average of 1 volume percent arsenopyrite but locally up
to 35%. Pyrite and pyrrhotite are also present. Arsenopyrite occurs
as 1 to 5 mm crystals that exist in or near quartz veins. Pyrite
occurs in veinlets, as irregular patches and/or as disseminations
in oxide and silicate iron formations. Pyrrhotite occurs as finely
disseminated grains.  In 1983 and 1984  prospecting and sampling
resulted in three gold occurrences (assays greater than 3 g/t Au)
being found in the Moth Valley area. See drawing 6601-203 from
Assessment Report #082134 for occurrence and sample sites. Dufresne
& Johnston, 1986 give the following results which are from 1983 and
1984 exploration:
Blaster gold occurrence (north of the west end of M Lake): A grab
sample of arsenopyrite bearing silicate iron formation assays 21.74
g/t Au, 180 to 600 m east along strike assays arsenopyrite bearing
oxide iron formation grab samples assay between 1.67 and 4.86 g/t
Au. These samples were collected from sulphide bearing iron
formation adjacent to crosscutting quartz veins. The sulphide
bearing zones are generally less than 3 m in strike length and less
than 1 m wide.  Moth gold occurrence(180 m NE of the east end of M
Lake): A grab sample from a 25 cm  by 2.5 m  arsenopyrite silicate
iron formation assayed at 3.38 g/t Au. West of this site three rock
samples from sulphidic zones of similar size and mineralogy assay
between 1.16 and 2.85 g/t Au.  Valley gold occurrence(approximately
250 m east along strike of the moth occurrence): Here the oxide
iron formation thickens to about 100 wide within a fold closure but
it contains numerous interbeds of greywacke and mudstone. The
sulphide bearing zones are generally less than 3 m in strike length
and 1 m wide. An arsenopyrite bearing sample assayed at 15.57
across 1.0 m. the zones are often coincident with abundant quartz
vein or silicified iron formation.  No ground exploration was done
in 1985.  Exploration of the area in 1986 consisted of prospecting,
sampling, and geological mapping at a scale of 1:5000. Two samples
were collected and assayed at 0.14 and 0.07 g/t Au.
No ground exploration was performed in the Moth Valley area between
1987 and 1989. In 1988 & 1989 Aerodat Ltd. performed airborne
geophysical surveys in the Needle Lake area.  Exploration in 1990
consisted of surveying a tie line, sampling and geological mapping
at a scale of 1:5000. Twenty rock grab samples and 17 rock
composite samples were taken from the siliceous shear zone. Assays
include a grab sample of 46.49 g/t Au and a composite grab sample
of 10.59 g/t Au across 0.25 m.
The Gollum Lake showing lies within the northeastern portion of the
the older lithologies.  The Gollum Lake showing is within the Back
are also present (Williamson and Olson,1990).  In 1988 &1989
Aerodat Ltd. performed airborne geophysical surveys in the Needle/
Gollum Lake area.  In 1990 reconnaissance prospecting, sampling and
mapping at a scale of 1:20,000 was done in the Gollum Lake area.
At Gollum Lake, there is a northeasterly trending, sulphide-bearing
shear zone within Beechey Lake Group sedimentary rocks adjacent to
a contact with a Regan Suite granitic pluton. The mineralized shear
zone can be traced for about 200 m, and is parallel to the contact
between Beechey Lake Group and the granitic pluton. The width of
the mineralized zone is undetermined due to poor exposure.
Disseminated chalcopyrite, arsenopyrite and pyrite in amounts up to
2 volume percent are localized within quartz-rich zones in
greywacke. Most of the samples which were collected have an
anomalous gold content. One rock grab sample that was collected
from chalcopyrite- and arsenopyrite-bearing greywacke along this
shear zone assays 14.09 g Au/t (Dwg. 0605.N-5)(Williamson & Olson,
1990).
The Gollum Lake North Showing consists of two samples that had gold
values above the database cutoff. It lies within the northeastern
dykes crosscut the older lithologies.  In 1988 & 1989 Aerodat Ltd.
performed airborne geophysical surveys in the Needle/Gollum  Lake
area.  In 1990 reconnaissance prospecting, sampling and mapping at
a scale of 1:20,000 was done in the Gollum Lake area.  A rock grab
sample from a pyrite-bearing quartz veins in silicate iron
formation, assayed 1.16 g/t Au, another sample assayed at 0.75 g/t
Au.
The Phaedrus Lake showing lies within the northeastern portion of
the Archean Slave Structural Province. The principal underlying
consist mainly of volcanics and metasediments.   The Yellowknife
major sequences. The Back Group is the lowest sequence and is
formation. The Showing is underlain by rocks of the Back Group.
Shears cut all rock types in the Phaedrus Lake area and locally,
along some of the shears the rocks are mineralized by gold bearing
sulphides.  In 1988 &1989 Aerodat Ltd. performed airborne
geophysical surveys in the Needle Lake area.  Rock grab samples
that were taken during 1990 reconnaissance prospecting and mapping
yielded gold values of 1.80 g/t Au and 0.54 g/t Au. These samples
were collected from chalcopyrite and arsenopyrite bearing quartz
veins within porphyritic andesite.
The North Jaeger Lake showing lies within the northeastern portion
of the Archean Slave Structural Province. The principal underlying
supracrustal rocks belong to the Yellowknife Supergroup and consist
mainly of volcanics and metasediments.  In 1988 & 1989 Aerodat Ltd.
performed airborne geophysical surveys in the Needle/Jaeger Lake
area.  The North Jaeger Lake showing consists of three rock grab
samples that assayed at 0.93 g/t Au, 0.88 g/t Au and 0.65 g/t Au.
These samples were taken during reconnaissance prospecting in 1990.
See dwg. 0606.N-10 from Assessment Report #082980 for the location.
No further data is available re lithology etc.
The BLS-3 showing lies within the northeastern portion of the
consist mainly of volcanics and metasediments.  In 1987 seven rock
samples were collected from the BLS-3 shear zone. These samples
assayed between 4.05 g/t Au and 22.77 g/t Au (Williamson & Olson,
1990). There was no assessment report found for this exploration,
the information is solely from the reference given.   In 1988 &
1989 Aerodat Ltd. performed airborne geophysical surveys in the
Needle Lake area.  Reconnaissance prospecting was done in 1990. One
sample taken approximately 650 m SE of the 1987 samples in a
siliceous greywacke ran 8.19 g/t Au.
The Feather Lake showing lies within the northeastern portion of
the older lithologies.  The Feather Lake showing is within the Back
Yellowknife Supergroup rocks in the area are folded into a steeply
dipping, NW striking, regional scale anticlinorium that plunges to
the SE.   The majority of the rocks that under lie the Feather Lake
area are greywacke mudstone turbidite sequences with interbedded
iron formation. Both oxide and silicate iron formations are present.
The oxide iron formation are up to 20 m wide and have well defined
bedding which include layers of massive magnetite to quartz
magnetite. The silicate iron formation are usually less than 5 m
wide, are poorly banded but are distinctive from other chloritic
unit by the presence of grunerite.  Two main oxide iron formation
layers are mapped in the Feather Lake area, both are 3-4 m wide,
well bedded, and folded to achieve an apparent thickness of 40 m. A
third narrow,discontinuous layer is noted in the Feather Lake area.
This layer varies from oxide to silicate iron formation along
strike.
Mineralization consists of chloritized iron formation with
disseminated pyrrhotite, pyrite and chalcopyrite. Arsenopyrite was
only noted in one area. Quartz veining with chloritic sulphidized
margins are rare. The majority of quartz veins are tension gashes
that are best developed in thick arenite or greywacke beds.   An
airborne magnetometer survey of NTS sheet 76G/03 was flown by the
GSC in 1968. In 1981 Frith compiled the regional GSC mapping of the
area in the GSC Open file.   In 1983 and 1984 Trigg, Woolletts and
Olson Consulting conducted limited reconnaissance prospecting.  In
1988 Aerodat flew an airborne magnetometer survey over the area,
the data indicated three discontinuous to continuous oxide iron
formations that form an easternly plunging, folded and faulted
synform (Williamson & Olson, 1989).    In 1989 exploration included
reconnaissance prospecting, sampling, grid surveying, mapping, and
ground magnetometer and VLF-EM surveying. Of 124 rock samples
collected, gold assays range from 0.07 g Au/t to 15.19 g Au/t. Two
samples had assays of 5.06 g Au/t and 15.19 g/t Au, 27 samples
assayed between 0.15 and 3 g/t Au. The samples that assay greater
than 0.15 g/t Au generally have greater than 4 volume percent
pyrite or pyrrhotite or both in association with quartz and
chlorite.  Drawing 9608.I-2 from assessment report #082854 gives
the sample locations and geology of the area.  In 1994, exploration
consisted of mapping and sampling of rock and till. Mineralization
was found to be spotty and of 362 samples collected, none assayed
greater than 10 g Au/t. Repeat samples taken from the the areas of
the 8 and 15.19 g/t Au assays from 1989 assayed 0.7 and 0.3 g/t Au.
Malley Rapids Sheet 2 from assessment report #083394 shows the
geology and sample locations.
The Bor Lake showing lies within the northeastern portion of the
the older lithologies.  The rocks that underlie the Feather Lake
area are greywacke mudstone turbidite sequences with sparse
outcroppings of interbedded iron formation. Both oxide and silicate
iron formations are present. The oxide iron formation are up to 20
m wide and have well defined bedding which include layers of
massive magnetite to quartz magnetite. The silicate iron formation
are usually less than 5 m wide, are poorly banded but are
distinctive from other chloritic unit by the presence of grunerite.
Exploration in the Bor Lake/Malley Rapids area has included:
Airborne magnetometer survey by the Geological Survey of Canada in
1968 of NTS map sheet 076G/03.  During 1983 and 1984 reconnaissance
prospecting and sampling were done with rock grab samples assaying
up to 0.3 g/t Au(Williamson & Olson, 1989).  In 1988 an airborne
magnetometer, VLF-EM and muilticoil, multifrequency electromagnetic
geophysical survey was done by Aerodat Ltd.  Exploration in 1989
involved reconnaissance prospecting, mapping, and sampling along
airborne magnetic anomalies or airborne electromagnetic conductors.
Assays listed are all under 0.3 g/t Au.  One sample from 1994
reconnaissance mapping assayed at 555 ppb. See Malley Rapids Sheet
4 from assessment report #083394 for locations.
The Bor Lake SE showing lies within the northeastern portion of the
mainly of volcanics and metasediments. Archean intrusive and
metamorphic rocks also underlie the region. Early Proterozoic
the older lithologies.  The rocks that underlie the Bor Lake SE
Exploration in the Bor Lake SE/Malley Rapids area has included:
up to 0.3 g/t Au (Williamson & Olson, 1989).  In 1988 an airborne
involved reconnaissance prospecting, mapping and sampling along
airborne magnetic anomalies or airborne electromagnetic conductors
in the area but no samples were taken from this particular site.
In 1994 the area was subjected to prospecting and sampling. One
sample taken from a  large outcrop of rusty quartz-grunerite-
chlorite iron formation that was crosscut by quartz veins and
sulphidized with pyrrhotite and pyrite had an assay of 601 ppb g/t
The Zone F showing lies within the northeastern portion of the
crosscut the older lithologies.  The Zone F showing is within the
are also present (Williamson and Olson,1990).  The rocks that
underlie the Zone F area are greywacke mudstone turbidite sequences
with interbedded iron formation. A mantle of quaternary glacial
material covers most of the area of Zone F. Sporatic exposure of
sulphidized oxide iron formation lies along a shallow fold hinge.
Exploration in the Zone F/Malley Rapids area has included: Airborne
magnetometer survey by the Geological Survey of Canada in 1968 of
NTS map sheet 076G/03.  During 1983 and 1984 reconnaissance
in the area. Samples assayed up to 0.48 g/t Au.   In 1994 this area
was mapped and resampled. Of 22 samples taken, one sample assayed
over 1 g/t Au. Other grab samples yeilded assays of 578 ppb, 637
ppb, 734 ppb and 758 ppb Au.
The Bee showing lies within the northeastern portion of the Archean
lithologies.  The Bee showing is within the Back River region. The
the SE. The Bee showing area is underlain by siltstones, greywackes,
mafic to intermediate volcanic rocks and minor mafic/felsic tuffs
that have been metamorphosed to mid greenschist grade.  Plate 2
from assessment report 081969 shows the rock types and
relationships.  The mafic, volcanic unit is about 400 m wide and
lies between siltstones to the south and greywackes to the north.
They consist mainly of sheared pillow basalt. Locally, where
shearing is more intense, these rocks are converted to chloritic
schists that are cut by carbonate veinlets. The tuffaceous rocks
outcrop sporatically within a 30 m wide draw near the upper part of
the mafic volcanic unit. This fragmental unit consists of
interbedded mafic and felsic tuffs with thin cherty and
argilliceous layers. The mafic tuffs are variously chloritized and
in places are now chlorite schist, containing up to 10%
disseminated opyrite. Felsic tuffs, usually containing 1-2 mm
diameter quartz eyes, occur in beds 1/2 to up to 5 m wide. They are
variously sericitized and in places they are sericitic schists, up
to 1 m in width, containing 5-10% disseminated to streaky pyrite
and minor arsenopyrite. It is within these pyritic, sericitic,
arsenopyritic-bearing schists (Main showing, Plate 2) that the best
gold values occur. Minor quartz veinlets occur throughout the Main
showing area, which is exposed over a strike length of about 100 m
before disappearing into a lake to the east and overburden to the
west. (Sorbara, 1985)
A GSC reconnaissance lake sediment geochemical survey was done in
in the Bee area as part of a larger study which sampled silts for
Cu, Pb, Zn, Ni, U, Mn, Fe, K2O and organics (Allan et. al., 1972).
In 1974 the area was mapped at a 1:50,000 scale and the area was
prospected for sulphide mineralization and in the area of a
granitic pluton for uranium. Geochemical sampling was done for Cu,
Pb, Zn, Ag , Au and As.  Sampling in 1974 did not result in any
anomalous samples within the Bee area.  1975 exploration included
geological mapping at a scale of 1inch = 1250ft, prospecting, rock
and soil sampling. One gold occurrence was discovered immediately
SW of Awm Lake within an interbedded unit of black slates and
chlorite schist which contained arsenopyrite and pyrite. The chip
sample assayed at 0.098 oz/ton Au across 10 feet.  1985 exploration
consisted of grid marking, geological mapping, trenching, rock
sampling, ground magnetics and VLF-EM surveys. Two samples from the
Main showing (See Plate 2 from assessment report # 091969) assayed
at 1,920 and 1,910 ppb gold respectively from a highly sericitic
felsic tuff that had streaky pyrite. 19 line km of ground magnetics
and VLF-EM were completed over the Bee (Main) showing. The magnetic
survey only delineated the diabase dykes. Four VLF-EM conductors
were found parallel to the strike of the stratigraphy. The
southernmost conductor is at least 2300 m long and occurs along a
mafic volcanic/siltstone contact, a conductor immediately to the
north is totally covered by overburden - no  explanation for either
was given.  The conductor coincident with the Bee (Main) showing
has a strike length of at least 1700 m. The northernmost conductor
does outcrop but no explanation was noted for same.
The Robbs Pond showing lies within the northeastern portion of the
the older lithologies.  Rocks underlying the Robbs Lake area are
mainly schists derived from a greywacke-mudstone sequence and
various facies of iron formation. To the south, a band of grey-
green non banded phyllites and fine grained mica schists were
mapped between the greywacke units.   A GSC reconnaissance lake
sediment geochemical survey was done in in the Bee area as part of
a larger study which sampled silts for Cu, Pb, Zn, Ni, U, Mn, Fe,
K2O and organics (Allan et. al., 1972).  In 1974 the area was
mapped at a 1:50,000 scale and the area was prospected for sulphide
mineralization and in the area of a granitic pluton for uranium.
Geochemical sampling was done for Cu, Pb, Zn, Ag , Au and As.  In
assessment report 061343, one Zn value of 0.54% was noted but not
located on the accompanying map. Two assays had gold values of 0.48
ounces per ton and 1.44 ppm respectively. These samples were
located 800 ft apart in bands or lenses of pyritic meta-chert
interlayered with amphibolite. No other anomalous results were
noted.  1975 exploration included geological mapping at a scale of
1inch = 1250 ft, prospecting, rock and soil sampling. No anomalous
samples were obtained from the Robbs Lake area.
In 1985 the area that the grab sample of 0.48 opt Au was taken in
1974 was resampled but no gold values of interest (sic) were found
and Sorbara, 1985 suggests that the original sample was misplotted.
The DOX 2380 showing lies within the northeastern portion of the
consist mainly of volcanics and metasediments.   Yellowknife
Supergroup rocks in the area are folded into a steeply dipping, NW
striking, regional scale anticlinorium that plunges to the SE.
Rocks underlying the sample area are mainly semi-pelite and pelite
(siltstone and shale) with chloritic interbands and various facies
of iron formation.   A GSC reconnaissance lake sediment geochemical
survey was done in in the Bee area as part of a larger study which
sampled silts for Cu, Pb, Zn, Ni, U, Mn, Fe, K2O and organics
(Allan et. al., 1972).  In 1974 the area was mapped at a 1:50,000
scale and the area was prospected for sulphide mineralization and
in the area of a granitic pluton for uranium. Geochemical sampling
was done for Cu, Pb, Zn, Ag , Au and As.  In assessment report
061343, one Zn value of 0.54% was noted but not located on the
accompanying map. No anomalous gold values were reported for this
area.  1975 exploration included geological mapping , prospecting,
rock and soil sampling. One anomalous gold value assayed at 0.018
oz/t.
The DOX 2384 consists of one sample that lies within the
northeastern portion of the Archean Slave Structural Province. The
region is bordered by the Aphebian age  Bear Structural Province to
the west, and the Rae Structural Province to the east. The
principal underlying supracrustal rocks belong to the Yellowknife
Supergroup.   A GSC reconnaissance lake sediment geochemical survey
was done in in the Bee area as part of a larger study which sampled
silts for Cu, Pb, Zn, Ni, U, Mn, Fe, K2O and organics (Allan et. al.
, 1972).  In 1974 the area was mapped at a 1:50,000 scale and the
area was prospected for sulphide mineralization and in the area of
a granitic pluton for uranium. Geochemical sampling was done for Cu,
Pb, Zn, Ag , Au and As.  In assessment report 061343, one Zinc
value of 0.54% was noted but not located on the accompanying map.
1975 exploration included geological mapping, prospecting, rock and
soil sampling. One sample from a silicate-oxide iron formation/
minor sulphide iron formation had an assay of 0.03 oz/t Au.
The DOX 2372 Showing consists of a single sample. It lies within
the northeastern portion of the Archean  Slave Structural Province.
The principal underlying supracrustal rocks belong to the Archean
Yellowknife Supergroup and consist mainly of volcanics and
metasediments.  A GSC reconnaissance lake sediment geochemical
061343, one Zinc value of 0.54% was noted but not located on the
accompanying map.  No other anomalous results were noted.  1975
exploration included geological mapping, prospecting, rock and soil
sampling. One anomalous sample from a pyritic iron formation had a
gold value of 0.02 oz/t.
The H-106 is a single sample showing that lies within the
region is bordered by the Aphebian age Bear Structural Province to
Supergroup and consist mainly of volcanics and metasediments.  In
1985 a reconnaissance mapping and prospecting program was
undertaken over an area that was covered by three prospecting
permits (PP1053, 1054 & 1055). A sedimentary stratigraphy was
identified that hosts amphibolitic iron formation over a 23 km
strike length. The sporatic amphibolite-magnetite iron formations
are locally cherty and rarely sulphidic. Both the bedding and the
foliation of the sedimentary package trend at 130-140 degrees with
moderate to steep NW dips. Of 143 samples taken, 6 assayed over 500
ppb Au.  In the showing area, one sample of undifferentiated iron
formation assayed at 690 ppb Au.
The F-74 showing is a single sample site that lies within the
Supergroup and consist mainly of volcanics and metasediments.   In
moderate to steep NW dips. Of 143 rock samples taken, 6 grab
samples assayed over 500 ppb Au.  In the showing area, one sample
of silicate/sulphide iron formation assayed at 522 ppb Au.
The K-97A showing lies within the northeastern portion of the
K-97A showing is within the Back River region. The Yellowknife
In 1985 a reconnaissance mapping and prospecting program was
samples assayed over 500 ppb Au.  The single sample that represents
this showing is from a felsic tuff/flow that outcrops in the SW
region of  PP1054. The sample site [ See Plate 2 (assessment report
081937)] is near a limestone/skarn contact area that  is adjacent
to the greywacke shale biotite schist sediment package.  In the
showing area, this single sample assayed at 580 ppb Au.
The K-117 & K-140 showing lies within the northeastern portion of
mainly of volcanics and metasediments.  In 1985 a reconnaissance
mapping and prospecting program was undertaken over an area that
was covered by three prospecting permits (PP1053, 1054 & 1055). A
sedimentary stratigraphy was identified that hosts amphibolitic
iron formation over a 23 km strike length. The sporatic amphibolite-
magnetite iron formations are locally cherty and rarely sulphidic.
Both the bedding and the foliation of the sedimentary package trend
at 130-140 degrees with moderate to steep NW dips. Of 143 rock
samples taken, 6 grab samples assayed over 500 ppb Au.  In the
showing area, two samples of silicate/sulphide iron formation
assayed at 1934 and 884 ppb Au respectively.
The Dior is a single sample showing that lies within the
principal underlying supracrustal rocks belong to the Archean
metasediments. Archean intrusive and metamorphic rocks also
underlie the region. Early Proterozoic (Aphebian) clastic
sedimentary and carbonate sequences of the Goulburn Group
lithologies.  Intruding the sediments is a 700 m by 400 m diorite
to quartz diorite stock. Near the eastern margin of the stock a
poorly exposed zone of arsenopyrite bearing quartz veins has been
traced for 700 m. The 2-3 m wide zone has 10-20% veins and veinlets
which generally carry 1% arsenopyrite. Silicified quartz diorite in
3-6 cm vein halos carry 3-4% disseminated arsenopyrite. One sample
from a quartz vein subcrop boulder with 2-4% blocky disseminated
arsenopyrite had an assay of 1,020 ppb Au. All other assays from
the quartz veins and adjacent silicified material assayed below 100
ppb Au.
The Sed showing lies within the northeastern portion of the Archean
age  Bear Structural Province to the west, and the Rae Structural
lithologies.  The Sed showing gold mineralization is within
arsenopyrite bearing quartz veins hosted by turbiditic argilliceous
greywacke.  Exploration on the Sed showing area consisted of
reconnaissance traverse followed by detailed mapping, sampling and
a geophysical survey consisting of VLF-EM and Total Field Magnetics.
Samples collected were assayed for multi element ICP as well as by
atomic absorption for gold.  The best gold value obtained from a
grab sample had 31,600 ppb Au. Five chip samples along a 100 m
strike length and across 3-4 m of quartz veining had gold values
between 155 ppb and 2,930 ppb. Accompanying arsenic values range
from 1,425 to 36,564 ppm.
The Gersdorffite showing lies within the northeastern portion of
the older lithologies.  The Gersdorffite showing  consists of
sediment hosted veins of massive gersdorffite with minor
chalcopyrite in quartz gangue. The mineralization is diabase
associated and within a zone approximately 30 m long and 2 m wide
ajacent to a NW trending diabase dyke. Sample 135-3 had Ni values
of 19.35%, Cu 0.44%, Pt 100 ppb and Pd 1000 ppb. Sample 804-3 had
values of: Ni 15.55%, Pt 260 ppb and Pd 570 ppb. Sample 804-4 had
values of: Ni 5.60%, Cu 0.19%, Pt 80 ppb and Pd 630 ppb.
Reconnaissance geological mapping and sampling was done in the
Gersdorffite showing area in 1985 at a scale of 1:31,680. Map 4/7
from assessment report 082070 shows the sample locations.
The Gaet showing lies within the northeastern portion of the
the older lithologies.  The Gaet showing is within the Back River
Within the showing area, five geological units have been mapped.
They are: 1)Lower amphibolite metamorphic grade sediments
represented by well foliated fine grained grey schists ranging from
metapellites to metagreywackes and metaquartzites. 2)Low
metamorphic grade sediments in the form of phyllites and lightly
metamorphosed greywacke. 3)Amphibolitic iron formation which have
five facies type:garnet rich iron formation, amphibole rich iron
formation, banded amphibole and chert rich iron formation, oxide
rich iron formation and sulphide rich iron formation. 4)Intrusive
granites and granodiorites and 5)A diabase dyke 20-50 m wide which
trends at 50 degrees north.   Mineralization occurs within the
sulphide rich (greater tan 5%) iron formation. Pyrrhotite is the
dominant sulphide followed by pyrite. Sulphides average 5% but may
be up to 30% locally.  Reconnaissance exploration was done in 1989.
Of 100 samples taken, 30 had gold values from 100-750 ppb. One grab
sample had an assay value of 1.47 g/t Au and the best chip sample
had a value of 650 ppb Au across 4 m.  In 1990 increasingly
detailed exploration was done in the area including the emplacement
of a 3 km by 2 km grid, mapping at a scale of 1:2500, trenching
and sampling (grab samples, channel samples and trench samples).
All 281 samples collected in 1990 were taken from iron formations.
Four values greater than 1 g/t Au were detected including two from
a trench that had values of 1.92 g/t Au and 1.46 g/t Au in sulphide
rich iron formation . A frost heaved boulder from another sulphide
rich iron formation yeilded a value of 3.67 g/t Au and one grab
sample from a garnet and amphibole rich iron formation with 5%
pyrite had a value of 1.10 g/t Au. 65 samples had assay values
between 100 and 890 g/t Au. All the rest had results less than 100
The Gaet 4 showing lies within the northeastern portion of the
Archean  Slave Structural Province.  The principal underlying
mainly of volcanics and metasediments. The Gaet 4 showing consists
of a single sample from iron formation that had an assay value of 0.
75 g/t Au over 2m.
Information from assessment report 081986 which consists only of 2
diamond drill logs . Mineralization occurs within an andesitic unit
that is sandwiched between volcanic sediments and has minor
sulphides.  No assays were above 30 ppb Au in DDH 84-02, three
samples had assay values above the cutoff range in DDH 84-01 and
these are as follows: A 2.5 foot section of andesite with trace
pyrite and arsenopyrite had an original assay value of 2380 ppb Au.
and a reassay value of 0.03 opt. Au. A 5 ft. section had 20% dark
quartz and minor arsenopyrite gave an original assay value of 780
ppb Au. and was reassayed twice with resultant values of 0.034 opt
and 0.34 opt Au. A 2.8 ft. section with 1% asp had an assay value
of 1080 ppb Au. and a reassayed value of 0.044 opt.
The Barrel showing lies within the northeastern portion of the
Intrusive rocks of Hudsonian age  and younger  diabase dykes
crosscut the older lithologies.  The Yellowknife Supergroup in the
The Barrel showing is underlain by Beechey Lake sediments. The
sediments contain horizons of dacite tuff offset by at least one
fault. There is an absence of banded iron formation, the oxides
present are scattered occurrences of magnetite. Anomalous gold
values are from sulphide-bearing sediments, often with quartz veins.
Of twelve grab samples, only one returned a value above 0.1 oz/ton
and four contained trace values.  The area has been subjected to
prospecting, grid emplacement and has been mapped at a scale of 1:
2500 with concurrent magnetometer and electromagnetic surveys.
The Algood showing lies within the northeastern portion of the
Aphebian age  Bear Structural Province to the west, and the Rae
The Showing area is underlain by Beechey Lake group metasediments
including argilliceous greywacke  turbidites, oxide magnetite iron
formation and tuffs.  Mineralization is associated with sulphides
and magnetite iron formation in gossan zones paralleling
schistocity. Sulphides are arsenopyrite and pyrite in vein type or
alteration zone quartz/chlorite rock.  The coarser the arsenopyrite
crystals, the higher the gold values.   Numerous NE trending faults
cut the area. The displacement of the faults is minor and is
generally left handed displacement. Faulkner, (1963) suspects that
the displacement is the primary controlling factor of the
mineralization. Where the faults intersect an argilliceous band,
the resulting chlorite amphibole alteration becomes a suitable
locus of deposition for auriferous sulphide minerals. The sulphides,
quartz and perhaps gold may have replaced the sheared chloritic
rocks adjacent to the faults.  Within the Algood Showing area there
are four locations that have been mapped, prospected, subjected to
geophysical surveys, and sampled. These areas are the #1 Showing
(approximately 3.5 km north of Fidler Lake), Alskne (approximately
2.5 km north of Fidler Lake), Fido (approximately 2.25 km north of
Fidler Lake) and Doc (approximately 2 km SE of #1 showing). Two of
the areas (#1 showing and Alskne) have been drilled.   The Algood
Showing area has been subjected to exploration since 1946 including
prospecting and mapping. In 1947 11 drillholes were drilled for a
total of 481 m. In 1962 the property was again mapped and a ground
magnetic survey completed. Five diamond drill holes were completed
on the Alksne occurrence. No further work was done until 1980 when
further ground magnetometer and VLF-EM surveys were completed as
well as 10 diamond drill holes (#1 showing) for a total of 408.7 ft.
At this time the core from 1947 was relogged and sampled as well.
In 1985 two grids were established within the showing area (Fido &
Don).
Ranges of assay values from the four areas within the showing are
as follows:  #1 Showing: A grab sample from 1963 had an assay value
of 2.79 opt Au. The best assays from the 1980  diamond drill
program include 0.22 opt Au/2.07 m, 0.48 opt Au/0.88 m, 0.16 opt Au/
5.5 m, 0.11 opt Au/4.1 m, 0.165 opt/0.73 m, 0.19 opt Au/0.43 m and
0.07 opt/2.3 m.  Relogging of drill core from 1947 yeilded the
following gold  results: 0.11 opt/1.5 m, 0.23 opt/1.5 m and 0.15
opt/1.1 m  Alksne: Drill results from 1947 include gold values of 0.
55 opt/3 ft, 0.66 opt/1.3 ft, 0.45 opt/3ft, 2.10 opt/3.2 ft, 0.64
opt/3.2 ft and 0.43 opt/3 ft.  Doc: A selection of grab samples
from the Doc grid include assays from 0.06 to 0.99 opt Au.  Fido: A
selection of grab samples from the Fido grid range from 0.14 to 0.
42 opt/Au.
The South Fidler Lake showing lies within the northeastern portion
The Back River Group is the lowest sequence and is comprised of
felsic to intermediate flows, tuffs and breccias. The Hackett River
Group overlies the Back and consists of  volcanic flows that range
from felsic to mafic, as well as tuffs and chemical sediments. The
The South Fidler Lake showing is located 2 km south of Fidler Lake
and is underlain by rocks of the Back River Group. The
mineralization is contained within the host rocks of gossanous
felsic to intermediate lapilli tuffs that have been altered to clay
and chloritized. Sulphides associated with the mineralization are
pyrite and arsenopyrite. Only 5% of the area has outcrop and and
additional 5-10% is frost heaved.  Exploration in the showing area
commenced in 1986 with reconnaissance mapping and prospecting at a
scale of 1:50,000. Four samples from the showing area had assays
ranging from 0.082 opt Au to 690 ppb (0.02 opt) Au from clay
altered andesite with a range of pyrite from 2-10%  In 1987
exploration consisted of geological mapping at a scale of 1:2500, a
VLF-EM and proton procession magnetometer survey, rock sampling and
one diamond drill hole was drilled. The VLF-EM survey outlined two
strong conductors, one is oriented at 320 degrees and has a strike
length of  350 m and dips steeply to the west. The second conductor
trends at 175 degrees, has no defined dip direction and is
interpretted as a shear or fault structure. The magnetometer survey
showed one high/low coupling coincident with a VLF conductor. This
target was drilled and yielded over 20 feet of pyritized argillite
but no assays were over 0.01 opt Au. Eight rock samples ranged from
0.12 opt Au to 0.02 opt Au.  The Showing area has been further
subjected to reconnaissance mapping, geochemical sampling
(including ICP and sediment sampling for heavy minerals) and
airborne geophysical magnetic and EM surveys to detect any features
related to kimberlite pipes. In 1992 exploration focused on
kimberlites with the primary focus being on reassessing airborne
data for potential kimberlite pipes. Prospective localities are
shown on the maps within AR 083086.
The Narrow Lake showing lies within the northeastern portion of the
and the Back River volcanic belts, which are generally spatially
separate, may be coeval in their upper parts (Williamson and Olson,
1990).  At least four periods of deformation have affected the
Yellowknife Supergroup. Metamorphic grade in the Back River Region
ranges from sub-greenschist to upper amphibolite facies.
The Narrow Lake showing is underlain by rocks of the Back River
Group which consist of shales and felsic to intermediate tuffs.
Mineralization occurs locally in sheared shales that have quartz
veinlets and pyrite +/- arsenopyrite.   The Narrow Lake showing has
been subjected to geophysical surveys (proton procession
magnetometer and VLF-EM), reconnaissance mapping and grid
establishment, geochemical sampling and in 1992 airborne data was
reinterpretted to look for potential kimberlite pipes (prospective
localities are shown on the maps within AR 083086).  Four samples
from frost heaved shale with quartz and pyrite +/- arsenopyrite
have a range of gold values from 540 g/t Au to 745 ppb Au. Three
other samples have  higher assay values that range from 0.520 opt
Au to 0.858 opt Au but these are are from rounded boulders that are
not in place.
The MG1showing lies within the northeastern portion of the Archean
belong to the Yellowknife Supergroup and consist mainly of
divided informally into three major sequences.  The Back River
The MG1 showing is within the Back River Group volcanics. The
entire area is very poorly exposed with only approximately 10%
outcrop.  Mineralization occurs within quartz filled fractures in
andesite. The surrounding country rock is not altered.   In 1986,
geochemical samples from prospecting and reconnaissance mapping
yielded gold values of 0.396 to 2.14 ounces per ton in three
samples.   In 1987 a  grid was established and more detailed
mapping and sampling were done.  Re-examination of the area of the
vicinity of the 1986 2.14 opt Au sample failed to uncover
significant mineralization. Only one sample had an anomalous gold
value of 0.102 opt Au from a frost heaved rock.        The Showing
area has also been subjected to reconnaissance mapping, geochemical
sampling  (including ICP and sediment sampling for heavy minerals)
and airborne geophysical magnetic and EM surveys to detect any
features related to kimberlite pipes. In 1992 the primary focus was
reassessing airborne data for potential kimberlite pipes.
Prospective localities are shown on the maps within AR 083086.
The  Grid 4 showing lies within the northeastern portion of the
the older lithologies.  This showing consists of 5 samples that
range from 585 ppb Au to 0.790 oz/t.  Three samples are from
strongly silicified boulders that are highly angular, abundant and
numerous suggesting that they are frost heaved.  These samples
(felsic boulders) are located on map 24 from assessment report
082625 as being within a black shale unit adjacent to a felsic
tuffaceous unit.   A large mineralized boulder that was sampled in
1986 gave assay results of 0.466 oz/ton (described as a cherty
shale with arsenopyrite) was relocated in 1987 and resampled and
yielded results of 0.79 oz/ton. This sample is located in different
areas on two separate assessment reports, for the purpose of this
showing the location from assessment report 082625 was used (See
map 24) as this sample is specifically discussed and was resampled
yeilding an assay value of 0.79 oz/t Au.   The Showing area has
also been subjected to reconnaissance mapping and airborne
geophysical magnetic and EM surveys to detect any features related
to kimberlite pipes. In 1992 the primary focus was reassessing
airborne data for potential kimberlite pipes. Prospective
localities are shown on the maps within AR 083086.
The  Grid 5 showing lies within the northeastern portion of the
River Group is the lowest sequence and is comprised of felsic to
The Grid 5 showing has been subjected to reconnaissance and
detailed mapping, prospecting, geochemical sampling, grid
emplacement and ground geophysical surveys including VLF-EM and
magnetometer.  In 1986 reconnaissance geochemical sampling of a
locally derived boulder gave a result of 0.41 oz/ton gold. The
poorly exposed area was then resampled and bedrock samples gave
anomalous results of 215 ppb to 0.052 oz/ton gold in three samples.
Further work in 1987 included sampling but no assays were above
the cutoff for this NORMIN database.  The Showing area has been
further subjected to reconnaissance mapping of glacial features,
sampling of drumlin and stream sediments and airborne geophysical
magnetic and EM surveys to detect any features related to
kimberlite pipes. In 1992 the primary focus was reassessing
The  Grid 2 showing lies within the northeastern portion of the
The Grid 2 showing is underlain by the Back River Group that
consists of felsic to intermediate tuffs and flows and intermediate
to mafic flows. Two types of mineralization are noted. The first
type occurs as a boulder train 5 m wide and 50-100 m long. The
boulders are gossanous and consist of mineralized smokey quartz
veins and shear zone material with 2-15% disseminated to massive
pyrite and  2-10% disseminated laths of arsenopyrite . Two samples
had assay values above cutoff (935 ppb and 720 ppb gold).
Additional minor shears are noted to the south, these are narrow 50-
100 cm wide and extend for 50-100 m in length. Two samples from
this area had gold assay values of 0.04 oz/ton and 730 ppb. The
second type of mineralization is a small occurance of disseminated
arsenopyrite and pyrite in a rhyolite flow. One sample from this
area had an assay value of 840 ppb gold.   Three diamond drill
holes were drilled into a VLF conductor. A magnetometer high was
also associated with the area drilled as were anomalous grab
samples up to 935 ppb Au. No assay values above cutoff were
recorded from the drill core results.  Work done on the showing
area consists of mapping (reconnaissance and grid), VLF-EM and
magnetometer geophysical surveys, geochemical rock and soil
sampling and diamond drilling. Further work has included
reconnaissance mapping of glacial features and airborne geophysical
The  Grid 3 showing lies within the northeastern portion of the
major sequences.  The Back River Group is the lowest sequence and
is comprised of felsic to intermediate flows, tuffs and breccias.
The Hackett River Group overlies the Back and consists of  volcanic
suggests that the Hackett River and the Back River volcanic belts,
which are generally spatially separate, may be coeval in their
upper parts (Williamson and Olson, 1990).  At least four periods of
Three samples comprise this showing, all are from gossanous
boulders that have up to 10% arsenopyrite associated with quartz
veining. Gold values are: 0.034 opt, 0.38 opt and 955 ppb. The Grid
3 Showing is underlain by Back River volcanics and volcaniclastics.
Mineralization of the showing is within gossanous quartz veined
frost heaved boulders from a possible shear zone that has a strike
length of approximately 50 m.  The showing area has been exposed to
various exploration techniques including reconnaissance mapping and
prospecting, ground VLF-EM and magnetometer surveys, grid
emplacement, and rock geochemical sampling. This area has also been
subjected to reconnaissance mapping and airborne geophysical
The  Kate Zone showing lies within the northeastern portion of the
mainly of volcanics and metasediments.   The Kate Zone showing is
underlain by sediments of the Beechey Lake Group.  Mineralization
consists of quartz veining with 1-8% arsenopyrite in a siliceous
and chloritized argilliceous greywacke. Of eight grab samples taken,
one had an anomalous gold value of 1.02 g/t.
The Showing consists of only one sample which had an anomalous gold
value of 0.75 g/t. This sample was from a gossan that contained 8%
pyrite-pyrrhotite. The sample was from the volcanic/sediment
contact that is marked by chert-sulphide exhalites and iron
formation.  The Twin Lake East showing is underlain by rocks of the
Back River Group which is a part of the Yellowknife Supergroup that
lies within the northeastern portion of the Archean Slave
Structural Province.
The Fire Showing consists of a single stream sediment sample that
had an anomalous gold value of 1650 ppb. It was taken from an area
within the northeastern portion of the Archean Slave Structural
Province. This area is underlain by volcanic and sedimentary rocks
belonging to the Yellowknife Supergroup.    The showing area has
been subjected to reconnaissance mapping, geochemical sampling
including ICP and sediment sampling for heavy minerals. Other work
done in the area included airbornel magnetic and EM surveys to
detect any geophysical features related to kimberlite. In 1992
exploration focused on kimberlites with the primary focus being on
reassessing geophysical airborne data for potential kimberlite
pipes. Prospective localities are shown on the maps within AR
083086.  Beach, esker, drumlin, stream and till samples were
collected for analyses which included heavy mineral concentrate
picking followed by electron microprobe analyses of potential
indicator minerals. After the preconcentration of heavy mineral
samples the -0.25 mm fraction was analyzed for 32 element ICP and
gold geochemical analysis.
The Syn showing consists of a single stream sediment sample that
had an anomalous gold value of 3840 ppb.  It was taken from an area
belonging to the Yellowknife Supergroup.    The Showing area has
done in the area included airborne geophysical magnetic and EM
surveys to detect any features related to kimberlite. In 1992
Beach, esker, drumlin, stream and till samples were collected for
analyses which included heavy mineral concentrate picking followed
by electron microprobe analyses of potential indicator minerals.
After the preconcentration of heavy mineral samples the -o.25 mm
fraction was analyzed for 32 element ICP and gold geochemical
analyses.
The A0902 showing consists of one grab sample from a quartz vein
with chalcopyrite and sphalerite  within a dacite tuff. This sample
had  a copper value of 2900 ppm and a zinc value greater than 10000
ppm.  The A0902 showing area  is underlain by a sequence of
andesitic flows interbedded with dacitic to rhyolitic tuffs,
lapilli tuffs and breccias believed to be part of the Back River
complex (Bryan, 1983). The area of the showing has been subjected
to reconnaissance mapping and sampling. All samples were assayed
for Au, Ag, Ni, Cu, Pb, and Zn
The A0865 showing consists of one sample from  quartz  with pyrite
within a dacite lapilli tuff. This sample had  an anomalous gold
value of 686 ppb.  The A0865 showing area  is underlain by a
sequence of andesitic flows interbedded with dacitic to rhyolitic
tuffs, lapilli tuffs and breccias believed to be part of the Back
River complex which lies within the northeastern portion of the
Archean Slave Structural Province (Bryan, 1983). The area of the
showing has been subjected to reconnaissance mapping and sampling.
All samples were assayed for Au, Ag, Ni, Cu, Pb, and Zn
The A0912 & A0913 Showing area  is underlain by a sequence of
complex (Bryan, 1983) which lies within the NE portion of the Slave
Structural Province. The area of the showing has been subjected to
reconnaissance mapping and sampling. All samples were assayed for
Au, Ag, Ni, Cu, Pb, and Zn  This showing consists of two samples.
Sample A0913 consists of a massive chalcopyrite vein in quartz and
had assay values of 2400 ppb Au and >10,000 ppm copper. Sample
A0912 is located approximately 525 m to the west and is a felsic to
intermediate brecciated tuff. This sample had an anomalous gold
value of 720 ppb. Both samples are within intermediate to felsic
tuffs.
The Uist lake showing is from a single sample collected during
reconnaissance mapping.  The sample was of silicate exhalite facies
rock with arsenopyrite grains. This sample has a gold value of 549
ppb.  The Uist Lake showing lies within the northeastern portion of
the Archean Slave Structural Province.  The principal underlying
consist mainly of volcanics and metasediments. Archean
intrusive
The DC Grid Showing lies within the northeastern portion of the
informally into three major sequences. The Back River Group is the
consists of volcanic flows that range from felsic to mafic, as well
as tuffs and chemical sediments. The uppermost sequence is the
Survey of Canada suggests that the Hackett River and the Back River
The DC Grid showing has been subjected to reconnaissance and grid
mapping, geophysical surveys - magnetometer and VLF-EM and
geochemical work. Only three grab samples have been collected for
analysis from this showing.  Geophysical results show two weak
conductors within the greywacke stratigraphy which were
interpretted as possibly being contact zones between greywacke and
slates. Silicate exhalite horizons were not well indicated by the
instruments. The magnetic survey indicated a zone which may be
silicate and oxide iron formation 50 m in width. Outcrop is sparse.
One reconnaissance sample was taken in 1982 but did not have gold
values above the NORMIN cutoff.  Only two samples were taken from
the area in 1985, both samples had gold values of 0.03 oz/
ton
The DC Grid showing lies within the northeastern portion of the
the older lithologies.  At least four periods of deformation have
facies.  The H Grid is underlain by siliceous and slatey greywacke
which is cut by small pegmatitic veins. Some of the higher gold
values are obtained from mineralized quartz veins spatially
associated with the pegmatite.   Reconnaissance mapping and
sampling from 1983 produced three samples with gold values of 8914
ppb, 17,486 ppb and 53,144 ppb.  Work done in 1985 included
geophysical surveys, grid emplacement and rock geochemistry. Of 16
samples taken, 8 have gold values that range between 0.02 and 0.36
oz/ton Au. No significant VLF-EM or magnetic anomalies occur on the
grid.
The As Grid showing lies within the northeastern portion of the
sub-greenschist to upper amphibolite facies.  The As grid is
underlain by greywackes, argillites and narrow bands of silicate
iron formation of the Beechey Lake group.
The As grid has been subjected to reconnaissance mapping and
prospecting, mapping at a 1:2500 scale, geochemical sampling, grid
establishment and geophysical surveys - both total field magnetics
and VLF-EM.  Reconnaissance sampling from 1983 yeilded no results
over 65 ppb Au.  In 1985 a grid was established over the area
following magnetometer and VLF-EM surveys and prospecting which
detected portions of iron formation that are conductive as well as
portions of the chemical seds that are oxide facies (>6200 gammas).
Thirty samples were taken from the As grid area, 7 had gold values
ranging between 0.02 oz/ton and 0.19 oz/ton.  3 samples had assay
values of 0.01 opt Au, the remainder of the samples had nil or
trace Au values.
The Soc showing lies within the northeastern portion of the Archean
Slave Structural Province in the Hackett River Greenstone Belt. The
Hudsonian age  and younger  diabase dykes crosscut the older
lithologies.  The Yellowknife Supergroup is divided informally into
three major sequences. The Back River Group is the lowest sequence
amphibolite facies.  The Soc showing is underlain by greywackes,
argillites, felsic to intermediate tuffs and oxide-silicate-
arsenopyrite iron formation.
The Soc Showing area has had two grids emplaced - the Soc and the
FFB(ID 076GSW0057) grid. See Figure 4 from assessment report 081789.
The Soc Showing has been subjected to geological mapping at a 1:
2500 scale, geophysical surveys (magnetic and VLF-EM), frost heave
sampling and drilling of 3 diamond drill holes totalling 263 m.
The geophysical surveys outlined the magnetic properties of the
iron formation which trends NW-SE with an average width of 75 m on
surface. the VLF-EM survey detected conductive portions of the iron
formation delineating the arsenide-sulphide bearing strata on the
Soc grid. The FFB grid did not have any conductive zones.  90 frost
heave samples were collected from the two grids, 70 on the Soc and
20 on the FFB.  On the Soc grid, 4 samples had gold values over 1.0
oz/ton (2.23 opt, 1.38 opt, 1.18 opt and 1.13 opt Au), 11 samples
had gold values ranging from 0.5 to 0.99 oz/ton, 32 samples ranged
from 0.1 to 0.5 oz/ton Au. The remainder of the samples had gold
values less than 0.1 opt.   Of 20 samples from the FFB grid 3
samples had gold values of 2.61, 1.30 and 1.02 oz/ton, 2 samples
had gold values ranging between 0.5 and 0.9 oz/ton, 10 samples
ranged from 0.1 to 0.5 oz/ton Au and the remainder had values below
0.1 opt.  The 3 drill holes intersected the silicate-oxide-
arsenopyrite facies iron formation and had the following elevated
gold values.  DDH SL-5-83 (FFB grid) had a 3 m interval with a gold
value of 0.09 oz/ton including a 1 m interval of 0.350 oz/ton.  DDH
SL-6-83 (Soc grid) had 2 intervals 1 m wide with gold values of 0.
09 and 0.05 oz/ton respectively.  DDh SL-7-83 (Soc grid) had one
interval 2.5 m wide with a gold value of 0.036 oz/
This showing is part of the Soc showing. For further information
and references see Normin ID #
076GSW0056
The Main showing lies within the northeastern portion of the
Archean Slave Structural Province in the Hackett River Greenstone
Belt. The region is bordered by the Aphebian age Bear Structural
Province to the west, and the Rae Structural Province to the east.
grade  ranges from sub-greenschist to upper amphibolite facies.
The Main showing is underlain by Archean greywackes, argillites,
felsic to intermediate tuffs and oxide-silicate-arsenopyrite iron
formation.
The Main showing area has had  two grids emplaced  along strike (NW-
SE) - the East Main and the West Main (ID 076GSW0059) grids. See
Figure 3 from assessment report 081789.  The Main showing has been
subjected to geological mapping at a 1:2500 scale, geophysical
surveys (magnetic and VLF-EM), frost heave sampling and 8 diamond
drill holes totalling 798 m.  The geophysical surveys outlined the
magnetic properties of the iron formation which trends NW-SE with
an average width of 75 m on surface. the VLF-EM survey detected
conductive portions of the iron formation delineating the arsenide-
sulphide bearing strata on the Main grid.  Surface geochemical
sampling yeilded the following results:  East Main grid had 51
samples assayed for gold. Two samples had values greater than 1 oz/
ton, 8 samples had gold values ranging from 0.99 to 0.5 oz/ton.
West Main grid had 41 surface samples collected, 3 had gold values
over 1 oz/ton, 2 of these samples are listed as being from 1982
(possibly from reconnaissance sampling though I cannot find an
accompanying report). 6 samples had gold values between the range
of 0.99 to 0.5 oz/ton.   Eight diamond drill holes were drilled as
well, 2 in the West Main grid and 6 in the East Main grid. Only one
drill hole, SL-10-83, did not encounter mineralization.
This showing is part of the Main showing. For further information
076GSW0058
The Fire 10 showing lies within the northeastern portion of the
Hudsonian age  and younger diabase dykes crosscut the older
lithologies.  At least four periods of deformation have affected
the Yellowknife Supergroup. Metamorphic grade  ranges from sub-
greenschist to upper amphibolite facies.  The Fire 10 showing is
underlain by Archean felsic tuffs with adjacent arenaceous
greywackes, slates, and intermediate volcanics.  Angular frost
heaved mineralized boulders of felsic volcanics extend over an area
of 25x75 m. These rocks are sheared and leached and contain
sphalerite, galena and pyrite. Reconnaissance mapping and
geochemical sampling has been done on the showing area.
Assessment report 082927 reports of reconnaissance mapping and
sampling from 1987 in which samples of felsic volcanics had the
following values: 1.92 oz/ton Ag, 420 ppb Au, 3.19% Pb, 7.81% Zn
(#17644 from AR 082625), 95 ppb Au, 1.05% Pb, 3.86% Zn (#17645) and
1.98 oz/ton Ag, 765 ppb Au, 3.68% Pb and 16.43% Zn (#17646).
Samples from the showing area taken in 1989 yielded the following
results: 1.1-35 ppm Ag, 21-600 ppm Cu, 550-24,400 ppm Pb and 75-71,
400 ppm Zn (#59867-59875).  This area has also been subjected to
further reconnaissance mapping and airborne geophysical magnetic
and EM surveys to detect any features related to kimberlite pipes.
In 1992 the primary focus was reassessing airborne data for
potential kimberlite pipes. Prospective localities are shown on the
maps within AR 083086.
The Uist 1 showing lies within the northeastern portion of the
Supergroup. Metamorphic grade  ranges from sub-greenschist to upper
amphibolite facies.  The Uist 1 showing is underlain by Beechey
Lake argilliceous greywacke turbidite sequences with silicate
facies iron formation horizons striking NNW.
Arsenopyrite +/- pyrite +/- pyrrhotite mineralization is hosted
within altered silicate iron formations which are noted over a
strike length of approximately 1.65 km (See AR 083045 Map 2). The
Uist 1 showing consists of two grid/showing areas called Wallys
showing and Eds showing.  The Uist 1 showing has been subjected to
prospecting, geophysical surveys (magnetometer & EM), geological
mapping, rock, soil and till sampling and grid emplacement.  In
1990 work done on the Ed showing included prospecting and
geochemical sampling with 10 samples collected. Eight of the
samples had gold values over 1g/tonne. The highest gold value
collected was 46.66 g/tonne.  Work in 1991 consisted of mapping and
prospecting at a scale of 1:10,000. Assay values of up to 46.66, 20.
64 and 11.28 g/tonne were returned from grab samples from Eds
showing. Values of up to 156.28, 63.22 and 10.01 g/tonne gold were
obtained from grab samples from Wallys showing.   In 1993 a soil
and till sampling program was carried out on the showing area
designed to evaluate the possible presence of kimberlite intrusions
to evaluate the diamond potential of the property. As well, rock
sampling was done to investigate precious and base metal deposit
possibilities. Eleven till and soil samples and 5 rock samples were
collected. No definate anomalies, indicator mineral suites or
geochemical signatures similar to those of kimberlite pipes were
discovered. No assay values are listed for the rock samples.
In 1994 work carried out on the Uist 1 showing area included
geophysical surveys, geochemical sampling and geological mapping.
A magnetic survey showed that the silicate facies iron formation
are adjacent and relate to a segment of a prominant oxide facies
banded iron formation that trends NW from Regan Lake. Locally the
BIF is deformed. The survey pinpointed the mineralized trend of the
IF.  An EM geophysical survey over the same area did not encounter
strong responses associated with wide sulphide rich BIF but number
of weak responses proximal to oxide facies iron formation were
present.  Sampling failed to identify zones of significant grade or
width. Of 13 samples collected, the highest gold grade was 0.04 oz/
ton gold.
This showing is part of the Uist 1 showing. For further information
and references see Normin ID # 076GSW0061.
The IM 1 showing lies within the northeastern portion of the
amphibolite facies.  The IM 1 showing is underlain by Archean
interbedded greywacke and amphibolitic iron formations consisting
of silicate, oxide and sulphide facies that trend northwesterly and
have a moderate to steep dip. The best gold values occur in
siliceous, amphibolitic iron formations containing pyrrhotite. The
greywackes are metamorphosed to biotite schists.
The IM 1 Showing includes the Triangle Lake Showing (ID 076GSW0064)
which is located along the same grid approximately 700 m SE. Work
done in the showing area includes reconnaissance mapping and
geochemical sampling ( including water samples for copper and zinc,
frost boil samples for copper, lead, zinc, silver and gold, and
rock samples for gold), geophysical surveys (including EM, VLF-EM,
magnetics), trenching and geochemical sampling and mapping of the
trenches.  Three samples  from reconnaissance work done in 1975 had
anomalous gold values of 1.05, 0.98 and 0.76 ppm.  Follow up work
done in 1976 included mapping at a 1:6000 scale, geochemical rock
sampling as well as soil and frost boil sampling and trenching (2).
Rock and soil samples were analyzed for copper, lead, zinc, silver,
and gold. Anomalous gold values from trenching are as follows: 0.
031, 0.028, 0.059 and 0.093 oz/ton gold.  AR 080576 reports
anomalous copper (2050 & 1050 ppm) and zinc(2300 ppm) values but I
am unable to locate these samples on the map provided.  No further
work was done on the showing until 1984 when the property was
reexamined. A grid was established and the area was subjected to
geological mapping, trenching, rock sampling, and geophysical
surveys including ground magnetics and VLF. The greatest
concentration of mineralization occurs in the vicinity of Triangle
Lake (see plate 2 AR 081970 for location) which has a sulphidic
zone approximately 500 m long. 73 grab and chip samples were taken
of amophibolitic iron formations. The best gold values (10,400 ppb
grab, 1,160 ppb/4 m chip and 1.090 ppb/6 m chip) are associated
with zones of bedded  pyrrhotite in siliceous, amphibolitic iron
The Triangle Lake Showing is part of the the IM 1 Showing (ID
076GSW0064) which is located along the same grid approximately 700
m NW. Work done in the showing area includes reconnaissance mapping
and geochemical sampling ( including water samples for copper and
zinc, frost boil samples for copper, lead, zinc, silver and gold,
and rock samples for gold), geophysical surveys (including EM, VLF-
EM, magnetics), trenching and geochemical sampling and mapping of
the trenches.  Three samples  from reconnaissance work done in 1975
had anomalous gold values of 1.05, 0.98 and 0.76 ppm.  Follow up
work done in 1976 included mapping at a 1:6000 scale, geochemical
rock sampling as well as soil and frost boil sampling and trenching
(2). Rock and soil samples were analyzed for copper, lead, zinc,
silver, and gold. Anomalous gold values from trenching are as
follows: 0.031, 0.028, 0.059 and 0.093 oz/ton gold.  AR 080576
reports anomalous copper (2050 & 1050 ppm) and zinc(2300 ppm)
values but I am unable to locate these samples on the map provided.
No further work was done on the showing until 1984 when the
property was reexamined. A grid was established and the area was
subjected to geological mapping, trenching, rock sampling, and
geophysical surveys including ground magnetics and VLF. The
greatest concentration of mineralization occurs in the vicinity of
Triangle Lake (see plate 2 AR 081970 for location) which has a
sulphidic zone approximately 500 m long. 73 grab and chip samples
were taken of amophibolitic iron formations. The best gold values
(10,400 ppb grab, 1,160 ppb/4 m chip and 1.090 ppb/6 m chip) are
associated with zones of bedded  pyrrhotite in siliceous,
amphibolitic iron formation.  For further information and
references see Normin ID # 076GSW0063.
The Orc showing is underlain by Archean volcaniclastics that strike
E-W and dip steeply to the north. Fold and fold closures give minor
evidence to tight isoclinal folding with the folds plunging
eastward. Mineralization  occurs within pyritic gossan zones hosted
in cherty rhyolite tuff and associated with acid fragmentals. Work
done on the showing includes: geological reconnaissance mapping,
soil sampling and a petrographic report of seven thin sections.
Four samples from a gossanous zone with minor disseminated
sphalerite and pyrite had zinc values of: 3400, 6000, 4400 and 4100
ppm.   Reconnaissance sampling from 1983 yielded assays with the
following range of gold, zinc, copper and silver values: 1.89 - 16.
7% Zn, 0.016 - 0.029 opt Au, 0.508 - 2.69% Cu and 1.49 opt Ag.
The Ray Showing is a small uranium showing exposed in Aphebian
gneiss and pegmatite over 29 meters at surface. Work included
airborne scintillometer, mapping and ground investigation of
anomalies in 1975-76. In 1978 a ground radiometric survey and
diamond drilling were completed. Indicated resources are listed as
75,000 at 1.00 lbs/t U3O8 to a depth of 60 m (1978). This showing
is small and did not continue at depth.
9 significant showings.
Turquetil Lake Northwest is a gold showing associated with
carbonate (-quartz) alteration within sheared mafic to intermediate
volcanics .  The host volcanic are part of the Archean Kaminak
Group supracrustral rocks in the Churchill-Hearne Structural
Province.  The alteration zone (shearing) is traceable in 4
seperate directions (north, northwest, southwest and southeast) for
up to 12 kilometres.  Gold mineralization has been encountered in
drill core on the eastern side of the  river in two carboante
altered, sheet-like zones which strike northeast and dip steeply
northwest (varying to north-northeast).  Gold mineralization in
these altered zones was encountered over a strike lenght of 940
metres.  On the western side of the Turquetil River a single gold-
bearing, carbonate altered (shear) zone occurs.  This zone is
traceable for about 1200 metres and is situated on the hanging wall
side of a northeast trending fault thats dips northward.   These
zones have alteration widths of up to 100 metres (DIAND,
Exploration Overview 1988; reference 1988).  Drill hole results
include 13.1 metres grading 7.27 grams/tonne gold and 8.5 metres
grading 9.21 grams/tonne gold.  A resource estimate was preformed
on the Turquetil Lake property with a probable resevre figure of 3,
800,000 tonnes grading 2.4 grams/ton which includes a drill-
indicated reserve of 550,000  tonnes grading 6.31 grams/tonne gold.
The zone is still open along strike and at depth.  A brief history
of the area starts with exploration work in the Turquetil Lake area
by Giant Yellowknife Mines in the 1960 s followed by geological
mapping completed in the 1970 s by the Geological Survey of Canada.
Essex Minerals Company, in 1976, intersected a gold-bearing zone
assaying 0.212 oz/ton over 43 feet during a drilling program.
Follow-up ground geophysicals was preformed in the late 1970 s,
along with additional diamond drilling.  Nobal Peak Resources and
Dejour Mines Limited, staked claims over the
mineralized
areas around Turquetil Lake.  Regional and detailed mapping,
diamond drilling, rock sampling (including channel sampling) and
airborne geophysics were used to better define the gold-bearing
structures since 1988.
The gold-bearing iron fromation comprising the Discovery prospect
occurs within the Archean Kaminak Group supracrustal rocks.  The
iron formation is along the Pyke Fault which extends for 50
kilometres (3 to 5 kilometres wide) through the Meliadine property.
Three structurally distinct  folds along the same iron formation
makes up Discovery which has a strike lenght of 250 metres and a
depth of 466 metres.  In 1989 the showing was first discovered
through sampling and geophysical means.  Since then tens of drill
holes and airborne geophysical surveys were used to better define
the showing.  The diamond drilling has yielded gold values of 19.89
grams/tonne  over 4.7 metres.  The showing is reported to contain 1,
386,000 tonnes of 6.8  grams/tonne gold (proven) and a probable
resource of 455,000 tonnes grading 6.47 grams/tonne gold.
The F-Zone is an cherty iron formation (magnetite-poor) with gold-
bearing quartz veins.  Theses quartz veins occur in the high
strained (fold hinges) areas of the structure.  A 4,300 foot strike
lenght is reported for the zone which is one of several iron
formations comprising the Wes Meg prospect.   Sulphide
mineralization in the iron formation includes mainly arsenopyrite
and [pyrite with lesser chalcopyrite.    Since at least 1994,  tens
of drill holes have been completed on the zone and an indentified
resource has been calculated based ion surface drilling results.
The indicated reserve for the F-Zone are 1,800,000 tonnes grading 7.
8 grams/tonne gold giving 0.4 million ounces of gold (reference
19980629Comaple).
The area is underlain by the easterly part of the Rankin - Ennadai
Greenstone Belt.  This belt, which is up to 380 km long, is
comprised of three east-northeast trending basins containing both
Archean and Aphebian rocks.  Archean rocks of the Kaminak
Supergroup (Lewry, Sibbald and Schledewitz, 1985) are comprised of
volcanic sequences, sediments and minor iron formation units.  At
least four complete mafic-felsic volcanic cycles are recognized
(Ridler and Shilts, 1974).   Recent mapping in the Tavani map area
has lead to further subdivision of the Kaminak Supergroup into the
Kasigialik Group and the Tagiulik Formation (Park and Ralser, 1990).
The Kasigialik Group encompasses a volcanic-sedimentary sequence
comprised of mafic pillow lavas (Atungag Formation), mafic and
felsic volcanics, volcaniclastics, breccias and conglomerates
(Akliqnaktuk Formation) and quartzofeldspathic turbidites
(Evitaruktuk Formation).  The Taguilik Formation is dominantly
quartz poor turbidites with banded ironstones.  Archean rocks in
the area generally trend northeast-southwest.   Kaminak Supergroup
rocks are unconformably overlain by Aphebian age sediments of the
Hurwitz Group which  form two elongate northeasterly striking
domains offset slightly by northwest trending dextral faults.  In
this area, Hurwitz Group is comprised of two main
ean D1 corresponds to large scale F1 folds, pervasive S1 foliation
and bedding parallel high strain zones.  D2, also Archean, is
characterized by northeast trending open to tight folds and steeply
dipping shear zones.  Proterozoic deformation, during the Hudsonian
Orogeny, resulted in the folding of both the Hurwitz Group and the
Kaminak Supergroup rocks.                    Age dating indicates
granite emplacement as syn-D1 and post-D2 (2659 +/- 4.6 Ma).
Metamorphism in Archean rocks varies from sub-greenschist to upper-
amphibolite near intrusive bodies, while Hurwitz Group reach sub-
greenschist facies.  A migmatite occurs in the western part of the
map area and is thought to have been thrust emplaced from the west
(Park and Ralser, 1990).                    Detailed mapping by Al
Miller of the GSC (Miller, 1989) divided the predominantly mafic
volcanic sequence into three meta-volcanic units with minor meta-
sedimentary units.  The entire sequence trends northeast-southwest,
dips northwest at 40? to 60? and is interpreted to be an upright
homocline.  The three volcanic units (V1-V3) are basically
comprised of pillowed and massive flows while the sedimentary units
may contain tuffaceous sediments, pyritic chert and black slates.
Park and Rasler (1990) mapped these rocks as belonging to the
Akliqnaktuk Formation of the Kaminak Supergroup.
The Fat Lake showing occurs in one of two quartz diorite (termed
the  Fat Lake  suite by Park and Ralser, 1990) sills characterized
by 5 mm to 10 cm sized feldspar crystals in a medium grained,
equigranular matrix.  The Fat Lake intrusion occurs at/near the
contact of the V1 volcanic unit and the S1 sedimentary unit (Miller,
1989).  Contacts of the Fat Lake sill are sheared while those of
the Caribou Horn intrusion,
further northeast, are not deformed.  The shears trend about 050?,
with related shears at 030?, and imply dextral movement.  The
shears are believed to be important to both gold mineralization and
in influencing the deposition of Proterozoic Hurwitz Group
sediments (Miller, 1989).                    Gold mineralization is
found in quartz veins in supplemental shears which may be up to 5 m
wide and 300 m long (Skillings, 1986; AR 081936).  Veins are
preferential to the quartz diorite sill and appear to die out
within meters of the contact with the surrounding mafic volcanic
rocks.  The quartz veins are generally 0.3 m wide and from 25 to
100 m long (AR 081936) and highly irregular (may be folded or
boudinaged) demonstrating several opening/filling phases (Miller,
1989).  Between two and four generations of quartz are recognized
(Skillings, 1985; Skillings, 1986).  Veins contain varying amounts
of carbonate, chlorite and disseminated pyrite, chalcopyrite,
sphalerite, galena and visible gold.  There are reportedly numerous
quartz veins in the area but four (#99 - #103) veins have received
the most interest.                    Alteration in the quartz
diorite consists of black chlorite associated with the quartz veins
and epidote-like discoloration of the intrusive between the veins
(Miller, 1989).  The shear zones are generally chloritized and
carbonitized.  Some alteration of the magnetite and titanite is
also noted in the sill.                    Gold mineralization is
dated as being Archean.  Park and Ralser (1990) state that the
auriferous veins are
Work on this showing reportedly occurred as far back as the 1940s
when Hudson Bay Mining and Smelting blasted trenches (AR 080406).
In the 1970s the property was covered by the IT claims and grab and
channel samples were collected from quartz veins and carbonate
shear zones by a Coniagas/Denison/J.A. Syme joint venture group.
The best value from their sampling was 2.85 opt Au and 0.61 opt Ag
over 1 foot.  At $100 per ounce price of gold, it was recommended
no further work be done as the gold in the veins was high grade but
not sufficient in size (AR 080406).  Borealis Exploration Limited
first examined the ground as part of the exploration program on
prospecting permit 1070 (just north of Fat Lake).  The showing was
then staked as the SUSAN claims and Borealis also obtained numerous
other prospecting permits in the 55K/4 map sheet to protect ground
for further gold exploration.  Borealis work history on this
particular showing and others in the area is somewhat confusing and
hard to decipher from the various reports and the following is a
brief summary, as best as can be determined for the Fat Lake
deposit.  In  1985, Borealis did detailed mapping and grab, channel
and pan sampling on the A grid or South Zone (not to be confused
with the South Gossan zone) of Fat Lake.  (The North Zone or B grid
actually refers to the North Occurrence (see NT MINFILE showing
055KSW0042).).  The best value came from sample 15 which contained
4.02 opt Au (grab).  They also did Max-min suveys but did not get
any anomalies however a magnetic survey delineated a response
coincident with a northeast-southwest trending shear zone.
Exploration work in 1986 consisted of more detailed mapping,
sampling, geophysical surveys
and
diamond drilling.  They did EM and magnetic surveys and outlined
an EM conductor under Fat Lake which was consequently drilled with
6 holes (593 m).  The holes intersected iron formation and shear
zones but no good gold values were returned from sampling (AR
082788).  Detailed mapping, trenching (not alot of details about
this) and channel sampling were also completed.  The best sample
returned a 6.8 gpt Au value but the width of the channel is not
known.  Forty-five holes were  then drilled on the Fat Lake showing
totalling 1586 m. The following year, 8 more drill holes were
completed on the Fat Lake site and with encouraging results they
decided to do some underground development.  Borealis drove a 70 m
decline shaft to the -17 m and drifted about 75 m along the length
of one of the four main veins (Vein 101) for underground mapping
and sampling.  Later that season, another 25 drill holes were
completed (1270 m ) with a best result of 14.3 opt Au over 1.10 m
from a vein named Sofyas Vein (not sure if this is one of the
original four veins numbered 99-103).  A test mill also opertated
for three days processing 150 tonnes of ore from Vein 101 (AR
082788).  In 1988, a 3 m by 3.5 m ramp was driven to the 960 (-40
m) level (AR 082788, 1988 Annual Report) and 56 samples were
collected from the walls of the ramp.  In addition, 8 drill holes
were completed for 1271 m.  Ore reserves were calculated based on
72 inclined holes drilled on the #99-103 veins (of which only 36
had acid dip tests) and reserves were only calculated for the four
main veins.  They calculated reserves of 13,895 tonnes at 15.03
grams/tonne Au (AR 082788, page 14).  In the same year, the 1988
Annual Report for Borealis Exploration Limited (released March 31,
1988)
sta
Gold mineralization within the Cache Zone is associated with pyrite,
quartz veining, structural features and alteration typical of
major producing gold deposits (Troupe et al., 1989).  The deposit
occurs in a conformable shear zone within an altered felsic to
intermediate volcanogenic unit adjacent to a contact with mafic
volcanic flows.  Diamond drilling established that gold
mineralization extends more than 200 m vertically, the width and
grade increasing with depth.  The gold is associated with
disseminated, euhedral pyrite.  Five parallel but distinct zones of
mineralization have been recognised.  Channel samples taken by
Noble Peak (1989) across a 1 m wide quartz vein gave average assay
values of 1.71 oz/ton gold over 4 metres.  The discovery channel
sample assayed 58.6 g/t gold across 4 m of quartz stockwork.  A
possible reserve of 364 000 tonnes grading 9.26 g/t gold was
indicated by the 1988 drilling program.  Four holes were drilled in
1989 in order to outline the extension of the Cache zone 100 m
below the 1988 holes.  It is now thought that the mineralized zone
plunges to the west, has a strike length of 250 m and a depth of
300 m (EMPR-GNWT, 1995).  Five grab samples were taken by D.A.
Irwin (1995) just 300 m south-southeast of the main showing of the
Cache Zone.  Assays show anomalous gold for four of the five
samples, with values ranging from 840 - 7560 ppb gold (Irwin, 1995).
In Dec. 1971 Pan Ocean Oil Ltd. estimated average width to be 6
feet of 0.46% U3O8.
The Tiriruniak Zone is a quartz-rich shear cutting iron formation,
basalts and sediments of the  Archean Kaminak Group.  Drill core
contains white mineralized quartz veins (possible stockwork)
containing ankerite, arsenopyrite and locally pyrrhotite.  The
mineralized zone contains significant gold assays which include 0.
98 oz/ton gold over 7.7 feet (1998 dirll hole 205).   Local chert-
rich  breccia zones were intersected in drill core.  The showing
consists of two parallel zones termed the Upper Contact and Lower
Shear.  A mineralized trend extending about 1 kilometre was
delineated with diamond drilling on the Upper Contact Zone.  A
resource calculation of 8,000,000 tonnes grading 11.1 grams/tonne
gold (identified reserve) was completed in 1998 (reference
Ground surveys and 12 diamond drill holes totalling 2234 feet cut
values in 1970.  Estimated 500 tons of U3O8 and 1000 tons of MoS2.
The Heninga Lake volcanogenic massive sulphide deposits are
situated within the Rankin-Ennadai greenstone belt in the Archean
Hearne structural province. Mineralization occurs as three discrete
lenses in ash tuffs of the Kaminak Group, near the top of Leggetts
(1980) Formation A, a sequence of interlayered intermediate and
felsic lapillistones, ash tuff, volcaniclastic sediments, crystal
tuffs and mafic flows or sills. The overlying Formation B comprises
a sequence of intermediate to mafic flows, flow breccia, ash tuff,
lapillistone, breccia, volcaniclastic sediments and minor oxide
facies iron formation. Layered rocks generally strike eastnortheast
and dip vertically or steeply to the south. Archean rocks have been
regionally metamorphosed to the greenschist facies except in
contact zones around some larger intrusive bodies, where a higher
grade is developed. Large scale NNE trending isoclinal folds are
the dominant structural influence in the vicinity of the deposits.
Three sulphide lenses occur in Member A4 of Formation A, a 50 - 150
m thick sequence of intermediate to felsic ash tuff and
lapillistone with lesser tuffaceous sediments and chert. The
Western Zone consists of a single, 3 - 4 m thick and 400 m long
lense, while the smaller Eastern and Central lenses are up to 3 m
thick and 90 m long. All three lenses thin rapidly laterally,
dividing into multiple narrow horizons of semi-massive to massive
sulphides interbedded with chert and ash tuffs.  The Central and
Western zones both consist of a stratiform, bedded horizon of
sphalerite, pyrite and minor galena with a central, relatively
structureless core of chalcopyrite, pyrite and minor pyrrhotite.
A discordant stringer sulphide zone within a sericite-quartz-
chlorite-carbonate alteration pipe underlies the massive sulphides.
The Eastern zone lacks a feeder pipe and is dominantly a horizon of
bedded sphalerite, pyrite, galena, chalcopyrite and tetrahedrite.
Drilling has established a reserve of about 5.5
million tonnes grading 9.0% Zn, 1.3% Cu, 67.0 g/t Ag and 1.0 g/t Au.
The Ferguson Lake Cu-Ni sulphide deposit is located in the Archean
Hearne Structural Province, part of the previously designated
Churchill Province. Mineralization is present as a 20 km long
sulphidic zone situated in an east-west trending package of mafic
volcanics sandwiched between various high grade ortho and
paragneissic terranes. The volcanic rocks have been metamorphosed
to upper amphibolite to granulite facies. Several syn to post-
tectonic gabbros and late syenite intrusives cut the stratified
rocks.  The most abundant rock type in the immediate vicinity of
mineralization is a medium grained mafic amphibolite containing 30 -
60% hornblende. No primary textures remain although a moderate to
strong subhorizontal lineation is present. Sulphide mineralization
occurs in a 50 - 200 m wide, medium to coarse grained hornblendite
subunit that has been interpreted as a metamorphosed ultramafic
sill within the amphibolites. It contains more than 60% hornblende,
plagioclase and minor garnet and locally displays modal banding
probably related to metamorphism. A moderate foliation or lineation
is often present.  The main sulphide zone generally occurs as a
single discrete horizon up to 10 metres thick but may locally
comprise a series of narrow parallel horizons. A strong gossan
marks the zone in outcrop. Mineralization consists of both
Stringer type mineralization is more continous, consisting of
stratabound veinlets of chalcopyrite, pyrite and pyrrhotite
comprising up to 10% by volume of the hornblendite. Amphibolite
immediately adjacent to sulphides is garnetiferous. Canadian Nickel
(Inco) carried out a large program of geophysics, mapping, diamond
drilling and bulk sampling in the early 1950s, eventually outlining
approximately 7.3 million tons grading 0.87% Cu and 0.75% Ni in the
main mineralized zone. The deposit was traced over a strike length
of 7700 metres and to a depth of about 250 metres. In 1987,
Homestake Mineral Development Company optioned the property and
sampled it for PGE. Samples of breccia style mineralization
contained from 50-700 ppb Pt and up to 5000 ppb Pd. Samples of
stringer style sulphides contained from 80-800 ppb Pt and 90-1200
ppb Pd. Sulphides also contain erratically anomalous levels of Co
(up to several hundred ppm) and Au (up to a few tens or hundreds of
ppb).
The Yathkyed Lake showing is an unconformity-vein type uranium
deposit at the margin of the Helikian Dubawnt Group sediments and
hosted in the underlying Archean tuffaceous and exhalative
sediments. The deposit is stratabound and is delineated as several
thin moderately plunging shoots within the interflow sediments.
Work was done in the showing area from 1975-1982 and included
airborne radiometric, magnetic and VLF-EM surveys, ground
scintillator, magnetic and EM geophysical surveys, geochemical
sampling, geological mapping and diamond drilling. The drill
indicated resources of 387,619 tons at 1.05% U3O8 plus  141,934
inferred  tons at 1.24%. The resources were outlined by diamond
drilling in an nearly vertical zone 3,600 feet long to a depth of
750 feet. It is stated that this deposit would be difficult to mine
without substantial dilution.
The Lone Gull showing is an unconformity related vein type deposit
located near the faulted margin of the Thelon Basin. Mineralization
is hosted in multiple lithologies. Archean feldspathic wacke and
minor pelite, Archean/Proterozoic W-Mo bearing porphyritic granite
and Dubawnt group syenitic dykes. The uranium mineralization is
close to the surface, down to 175 m and is amenable to open pit
mining.  Work on the showing commenced in1974 with the initial
field geochemical and geophysical discovery. This was followed by
diamond drilling, a biological study, geological mapping,
geophysics, geochemical sampling, a gravity survey and in 1988-89 a
feasibility study.   The calculated resource for this showing is
listed as 2.99 million metric tonnes at 0.61% U3O8.
Mineralization of the Lost Lake showing is syngenetic but
remobilized uraninite dissemination within thinly interbedded
arkose-siltstone-mudstone of the upper Aphebian Amer group. The
showing is near the Thelon unconformity and this Aphebian
mineralization may have been upgraded by processes similar to
unconformity related vein type uranium mineralization.  Work on the
showing commenced in 1977 with a VLF-EM and IP geophysical survey
and geochemical sampling. in 1979 diamond drilling was done and in
1984 geochemistry, and a VLF-EM and magnetic geophysical survey was
completed. An inferred resource of 900,000 metric tonnes at 0.104%
U3O8 is listed.
The Third Portage Lake deposit lies within the Tehek-Sissons
greenstone metasedimentary belt of Archean age, in the Churchill
Structural province of the Canadian shield.  The belt is subdivided
into two groups and one, the Woodburn Lake group, underlies the
area of interest.  It is comprised of a northeast-trending sequence
of metavolcanic and metasedimentary rocks (Hauseux, 1989).  This
supracrustal package is dominated by fine-grained clastics such as
greywacke, argillite and rare pelite, but is characterized by the
presence of spinifex-textured komatiites and ultramafic schists,
oxide and silicate facies iron formations and associated quartzite
units (Hughes and Legault, 1993).  Rocks of the Woodburn Group are
intruded by Kenoran-age (late Archean) unfoliated granitic plutons
and Early Proterozoic-age Amer Group and Hurwitz Group supracrustal
rocks rest unconformably on the granties to the northwest and
southeast, respectively (Hughes and Legault, 1993).  Metamorphic
grade is generally upper greenschist but locally reaches
amphibolite facies.  The regional structure involves a large shear
zone and complex folding.  The shear zone is typified by brittle
features such as fault gouge, breccia and quartz veins in the north
and mylonitic features indicative of more ductile deformation in
the south.  The Portage Fault Shear Zone trends roughly north-south
and dips moderately to the west.  Four phases of folding have been
discerned in the area (Hughes and Legault, 1993).  Two phases have
been seen in drill core.  The first is isoclinal with tight folds
on the order of 10-20 cm across.  These are folded by a more open,
asymmetrical set of folds (Hubacheck and Atkinson, 1993).
Hughes and Legault (1993) argue that the entire supracrustal
sequence has undergone significant isoclinal folding and lies
within a regional recumbant fold structure.  The Portage Fault
Shear Zone (or Third Portage Lake Fault Zone) post-dates the
folding phases and may represent the gold fluid conuit for the
known mineralization (Hughes and Legault, 1993).  Significant gold
mineralization occurs in two settings.  Pyrrhotite-bearing ductile
shear zones in magnetite-chert-grunerite iron formation is the most
common type of mineralization.  However, higher grade gold
mineralization occurs where pyrite has been introduced, either as
direct replacement of previously folded pyrrhotite and magnetite or
in association with various quartz vein events.  This high grade
gold may be related to fold axes (Hubacheck and Atkinson, 1993).
Some of the highest grade assays are contained in sections having
20-50% grey quartz with pyrite,  Values up to 20.5 g/t over 4.8
metres were returned from 1989 drilling on the Third Portage Lake
deposit (Barham and Mudry, 1990).  Work has continued on the Third
Portage Lake deposit, which has been estimated to hold a resource
of over 710 560 oz of gold within 95 metres from the surface, at an
average grade of 6.53 g/tonne (cut).  Recent engineering studies
indicat that >90% of the resource will likely be accessible by open
pit extraction (Cumberland Resources Annual Report, 1996).
and dips moderately to the west.  Mineralization at the Third
Portage Lake North Extension is represented by a UTEM conductor and
mineralized frost heave at the surface.  Drilling confirmed
suspected anomalous gold associated with iron formation and
shearing.
A sequence of drill core comprising cherty iron formation and
quartz/muscovite-schist with pyritic and chloritic quartz veins
gave a gold of 9.2 g/tonne over seven metres (Hubacheck and
Atkinson, 1993).  The 1996 Annual Report for Cumberland Resources
Ltd indicates that the North Portage deposit holds a reserve of 259
185 tonnes gold grading 9.31 g/tonne for a total of 77 606 ounces
gold.
The Goose Island prospect is located just one km south of Third
Portage Lake deposit, which lies within the Tehek-Sissons
and dips moderately to the west.  Extensional drilling on Goose
Island confirmed the presence of a significant gold bearing horizon
located 1 km south of the Third Portage Lake showing.  Initial
prospecting and mapping in 1989-90 returned anomalous assays
ranging from 1 g/tonne to 16.7 g/tonne hosted in sulphidized iron
Follow-up geophysics in 1989 and 1991 indicate a strong, consistent
magnetic anomaly with moderate conductivity.  In addition, the 1991
UTEM and magnetics survey reveal the presence of a steeply dipping
conductive zone flanking the western side of the magnetic trend,
slightly offshore from the Island.  Four holes were diamond drilled
on Goose Island in 1991 and best results were returned from a
section having 20 - 50% grey quartz with pyrite and pyrrhotite (482.
4 g/t over 1 metre) (Hubacheck and Atkinson, 1993).  The 1996
Annual Report for Cumberland Resources indicates a reserve of 976,
834 tonnes grading 11.46 g/tonne gold.  The tonnage was calculated
over 37 drill holes on 50 metre line spacing with a 5 g/tonne cut-
off over a minimum of 2 metre core length.
The Eclipse lead-zinc prospect is situated about 26 km northeast of
the Polaris Pb-Zn mine on Little Cornwallis Island. It is one of a
number of Mississippi Valley type Pb-Zn deposits occurring in the
Cornwallis Lead Zinc district. In this district, mineralization
typically occurs in a paleokarst surface developed at an Early
Devonian unconformity within Ordovician to Silurian limestones of
the Thumb Mountain Formation. The presence of colloform sphalerite
in Devonian conglomerate clasts supports a Devonian age for
mineralization.  The main lithologies at the Eclipse deposit are a
light grey to brown, sublithographic limestone with abundant shaly
partings, contributing to rapid mechanical breakdown, and a buff to
brown dolomite with common traces of disseminated marcasite.  At
least three separate mineralized zones are located along a 2.5 km,
northerly trending axis of deformation marked by alignment of
cherty rubble patches as well as coincident geochemical and IP
anomalies. The northernmost is the largest and consists of two
major zones known as the West and East Breccias. Sulphides in the
West Breccia occur mainly as massive open space fillings in a fault
breccia with a gangue of white, coarsely crystalline calcite and/or
dolomite. Sphalerite is the dominant ore mineral and is generally
colloform-textured with alternating lighter and darker bands.
Galena is abundant locally as irregular crystalline blebs but is
erratically distributed. Both minerals are also found as
disseminations adjacent to massive sulphides, as weak replacements
of breccia fragments and as narrow, irregular fracture fillings.
The East Breccia is similar but of somewhat lower grade. One area
within this zone contains more abundant galena, in places as
colloform aggregates or layers up to 1 m thick.
An unusual, coarse grained calcite-dolomite rock described as
having white/greenish gray salt and pepper texture was noted in
many places in both zones. Disseminated crystals of sphalerite and
galena and colloform aggregates of sphalerite are distributed
throughout this rock type, which is not correlatable between holes.
In contrast to the Polaris deposit, little marcasite or pyrite is
present.  Except for slight secondary dolomitization of some
breccia fragments, little or no alteration is present. Contacts
between mineralization and wall rock are sharp and well-defined.
However, up to a third of the sphalerite to the drill-tested depth
has weathered to smithsonite.  The Centre and South showings occur
in narrow breccia zones paralleling the strike of the enclosing
dolomites. Angular fragments up to 8 cm in size are cemented with
white calcite and/or dolomite. Sphalerite and galena occur in the
matrix. Little additional information is available.  Work done on
the showing area from 1960-1972 included sampling, diamond drilling,
geological mapping, soil geochemistry, and a gravity survey.  Two
zones had resources calculated: The West Breccia zone: 1,000,000 t
at 12.43% Zn and 2.18% Pb to 50 feet and the East Breccia zone: 170,
000 t at 3.6% Zn, 0.5% Pb plus 265,000 t at 3.45% Zn and 2.19% Pb.
The Nickel King deposit is associated with an Early Proterozoic
mafic to ultramafic sill on the order of 60 metres thick. The sill
intrudes feldspathic to quartzose paragneisses containing granitoid
and pegmatoid segregations. Similar segregations in the sill
suggest that it predates granulite facies regional metamorphism.
Subsequent tectonism, probably coeval with metamorphism, has
deformed the sill into a tight to isoclinal fold, the axis of which
trends westerly and plunges westerly at about 14 degrees. The two
fold limbs dip to the south at 30 degrees and 50 degrees. Two
northerly trending, west-side-down faults offset the limbs of the
fold.  The sill is highly heterogeneous and includes norite, gabbro,
olivine gabbro and pyroxenite. It is altered in places to a
fibrous amphibole, probably actinolite or cummingtonite, along with
chlorite and biotite. Sulphides occur as irregularly distributed
disseminations to semi-massive segregations in the sill and are not
necessarily associated with alteration. Drill information suggests
that total sulphide content increases towards the nose of the fold.
Sulphide minerals are mainly pyrrhotite and chalcopyrite.
Pentlandite, often partly altered to a bravoite series mineral,
tends to occur as inclusions, bands and flame-like exsolutions in
pyrrhotite.  Cu and Ni grades tend to be higher in the lower limb.
A reserve has been estimated (AR 082812) at 4.9 million tons
grading 0.72% Ni and 0.19% Cu. Up to several hundred ppm Co and 200
ppb Pd are present in selected samples. Pt values are rarely above
a detection limit of 20 ppb.
The Dussault uranium prospect on the west shore of MacInnis Lake is
situated within Aphebian sediments in the Nonacho Basin, an
intermontane basin perched on Archean basement rocks of the Rae
Province. Mineralization consists of stratabound veins,
disseminations and aggregates of pitchblende that are restricted to
a 10 m thick unit or zone of interbedded arkose and siltstone/shale,
apparently within the Taltson Formation. Individual veins are up
to 5 mm thick but are generally much narrower. Chloritic alteration
is closely associated with pitchblende. Pyrite occurs in quartz and
calcite stringers with pitchblende and also as disseminated cubes
in the wall rocks. Other associated minerals include hematite,
chalcopyrite and galena. Secondary U minerals are developed at the
surface on high grade veins.  The main mineralized zone has been
traced for 150 m along strike, to 60 m at depth and is generally
between 0.5 and 2.0 m thick. Strike and dip are approximately 030
degrees and 50 degrees east respectively.  Mineralization rakes to
the NNE at about 40 degrees. Canadian Pipelines and Petroleum Ltd.
drilled 50 holes totalling 5194 m in the zone in 1955 - 56 and
outlined 27,000 tonnes grading 0.17% U metal.
The OConnor Lake quartz vein-hosted sulphide deposit occurs in a
medium to high grade metamorphic terrane within the Taltson
magmatic arc. Lithologies in the general area of mineralization
include metasediments, amphibolites, sillimanite-garnet gneiss and
quartz-biotite schist. Numerous other quartz veins, some of which
also contain base metal sulphides, are present in the area.  The
MWK #1 vein cuts an amphibolite band where it is exposed at surface,
trending northwesterly with a dip of 65 degrees to the southwest.
Its width varies between 0.5 and 2 m and averages about 1.5 m. Its
contacts are relatively sharp although minor quartz veins and
stringers in the wall rocks, averaging 15 cm in thickness, parallel
the main vein. A thin seam of graphite occurs at the footwall
contact. Sphalerite and galena are disseminated throughout the
quartz together with lesser pyrite and pyrrhotite. Pyrite and
chalcopyrite are abundant locally. Larger masses of sphalerite and
galena tend to occur near the vein margins and most exploration
work has concentrated on several shoots of this material, which
tend to pitch at 50 degrees to the northwest in the plane of the
vein.  Drilling and underground drifting have traced the
mineralized zone over 200 m in strike and to a depth of about 80 m.
A drill-indicated reserve of 67,950 tons grading 7.64% Zn, 3.12% Pb,
0.13% Cu and 0.29 oz/ton Ag has been established.
The Salkeld Lake Cu-Ag occurrence is situated within the Nonacho
Basin, an Aphebian intermontane basin perched on high grade Archean
basement rocks of the Rae structural province. The Nonacho Group
sediments comprise a sequence of freshwater clastic sediments
including mainly arkose with lesser conglomerate, siltstone, shale
and sandstone. All Aphebian rocks have been metamorphosed to the
lower greenschist facies with development of phyllite and some
granitization near intrusions. The area is intensely faulted and
complexly folded, with many superimposed deformational events.  The
immediate vicinity of the Salkeld Lake occurrence is underlain by
banded biotitic granite gneiss which is cut by red granite to
syenite. The red granite is commonly fractured and contains locally
abundant milky white quartz veins constituting up to 50% of the
rock. Unconformably overlying the gneiss/granites, are the lower
three formations of the Nonacho Group comprising mainly
conglomerate, arkose and greywacke.  Two mineralized zones occur at
or near the contact between sediments and basement gneisses. The
Stockwork Zone comprises fine disseminations and fracture-fillings
of bornite and chalcopyrite near sheared zones in gneiss, arkose
and conglomerate. Sheared zones are typically up to a metre wide,
schistose and contain abundant malachite and azurite. Generally
weak but locally intense silicification, biotitization and
hematization are present as well as fracture-controlled fluorite.
Anomalous elements include mainly Cu and Ag with lesser Zn, Pb, Mo,
Bi and Au.
The Shear-Hosted Zone is a large zone of shearing, fracturing,
silicification and quartz veining marking the contact between red
granite and overlying sediments. It is exposed over more than 200
metres and is up to 40 metres wide locally. Disseminated
chalcopyrite and bornite occur near the margins of higher-grade
shears. Within the broad contact zone and sub-parallel to the
granite-sediment contact, is a 10-30 metre wide sub-zone of intense
quartz veining and silicification. Where this is intersected by
shears, there are quartz breccias up to 5 metres wide mineralized
with massive chalcocite and lesser amounts of bornite, sphalerite,
chalcopyrite, galena and tetrahedrite. Smaller quartz veins locally
containing clots of chalcopyrite together with fractures containing
sphalerite, galena and chalcopyrite are also present.  Two minimum
reserves based on earlier drilling were calculated by Fortune
Minerals. A 150 ft wide portion of the Stockwork Zone was drilled
on 50 ft centres and contains a reserve of 64,400 tons grading 0.
63% Cu. A reserve of 59,000 tons grading 1.42% Cu and 1.74 oz/ton
Ag was calculated for a 550 ft strike length of the Shear-Hosted
zone to a depth of 100 ft.
The BBX Cu-Ag-Ni-Co prospect occurs in Aphebian Great Slave
Supergroup rocks within the Great Slave Basin or Fold Belt. Copper
mineralization is associated with a 1870+/-15 Ma basaltic diatreme,
one of seven volcanic centres in the vicinity of Taltheilei Narrows
that intrude sediments of the Great Slave Supergroup. The diatreme
consists mainly of accidental fragments of mafic volcanics, and
lesser sedimentary and granitic rocks set in a matrix of finely
comminuted rock debris. Juvenile volcanic material is thought to
represent less than 25% of the diatreme by volume.
Mineralization at the BBX prospect is thought to be the result
of several phases of activity. An early phase involved the
deposition of Fe-Co-Ni sulphides and sulpharsenides such as
gersdorffite, arsenopyrite and glaucodot. Later phases saw the
deposition of chalcopyrite, galena, barite and specularite. These
minerals occur as disseminations in the matrix of the diatreme, and
in fractures and veinlets cutting both matrix and fragments. A last
phase involved the development of quartz-carbonate veins.
In general, the diatreme exhibits pervasive chloritic
and carbonate alteration, both probably related to deuteric
processes. Hematitic alteration took place at the time of
emplacement. Potassic alteration involving the development of K-
feldspar and sericite is intimately associated with metallic
mineralization.  Work commenced on the BBX showing in 1948 when it
was staked, trenched and diamond drilled. It was again drilled in
1956. From 1971-1974 the area was subjected to geological mapping,
geochemical sampling, IP and magnetic geophysical surveys and
diamond drilling. A resource was calculated at 5,000 t at 6.13%
copper and 2.6 oz/t silver.
The Sachowia Lake Ni-Co-Bi deposit area is underlain by Archean
Yellowknife Supergroup rocks, including mafic flows and fragmentals
together with metasediments. A large granitic intrusion is present
to the north; various small granite pegmatite and aplite dykes
within the layered rocks are probably related to it. Ferruginous
sediments and lava flows of the Kahochella Formation (Great Slave
Supergroup) overlie Archean basement approximately 1 km south of
the occurrences.  Niccolite, skutterudite, gersdorffite,
rammelsbergite, arsenopyrite, pyrite and chalcopyrite occur in
structurally controlled quartz-carbonate veins and vein breccias.
The latter are generally less than 1 m in width but locally swell
to 3 m. Metallic mineral content varies considerably within the
veins, with one 1958 drill hole intersecting approximately 1 m of
massive niccolite.
spaced lenses interbedded with and grading into
optioned to Ego Resources.                         The Kennedy Lake
Zone which lies under Kennedy Lake is described in AR 061728 as the
western extension of the BB zone although it is separated from the
latter by a barren zone.  The zone is not exposed at the surface
although drilling outlined it to be 120 feet long with a maximum
width of 21 feet.  The ore is similar in all respects to that of
the BB zone.  Reserves for the Kennedy Lake zone were calculated at
43,000 tons grading 7.3% Zn, 1.1% Pb and 4.0 oz./ton Ag.
Resources Ltd. in the early 1980 s, who still held the claims in
The area is underlain by Archean greywacke, mica schists, and
quartzite of the Yellowknife group intruded by Archean age granitic
rocks.  Proterozoic diabase and gabbro dykes intrude the earlier
Archean metasedimentary and granitic rocks.  Within the main claim
block area kimberlite pipes are the only Phanerozoic age rocks
known.  Minor amounts of metasedimentary rocks occur within the
claim area and mostly comprise thinly bedded metagreywacke outcrops
with small rafts of migmatite.  At least 5 types of granitoid
intrusive rocks occur.  A large, homogeneous pluton of equigranular,
medium grained quartz diorite occurs in the south-central portion
of the main claim block and comprises plagioclase, biotite,
hornblende, quartz and epidote.  The pluton is weakly deformed with
poor foliation development.  Hornblende plus biotite tonalite and
biotite tonalite are obseved to intrude the metagreywackes and have
weak to strong foliations.  The two most voluminous granitoid rocks
present in the main claims block area include a distinctive two
mica granite and porphyritic biotite granite.  The two mica granite
typically comprises equal proportions of quartz, plagioclase and
potassium feldspar with 5 - 10% muscovite and biotite.  Apatite and
tourmaline are common.  These granites are fine to medium grained
and generally equigranular.  A tourmaline bearing pegmatitic phase
forms dykes and small stocks up to 250 m in diameter.  The two mica
granite intrudes greywacke and both tonalite units.
Diabase dykes are common in the main claims block area and post
date the granitoid rocks.  Diabase dyke swarms present within the
claim area include the McKay dyke, Contwoyto dyke swarm, Lac de
Gras dykes, Mackenzie dyke swarm and 305 dykes.  At least 26
kimberlites have been discovered within the main claims area and
post-date the granitoid rocks and diabase dykes.  The kimberlite
pipes have undergone minimal erosion as evidenced by preservation
of crater eqiclastic sediments.  The kimberlites are typically
several hundred metres in diameter, occur within glacially formed
lakes and are overlain by 5 to 30 m of sand and gravel.  Varieties
of kimberlite distinguished in drill core inlcude epiclastic,
tuffisitic and tuffisitic kimberlite breccia phases and massive
hypabyssal kimberlite.  Glacial deposits are varied and include
trunk and tributary esker ridges, drumlin-like boulder clay hills
and till sheet(s).  Glacial erosion has rounded, grooved and
polished the bedrock.  Till is the most common surficial sediment
identified in the Lac de Gras area.  A single till sheet attributed
to Late Wisconsinan Laurentide Ice represents several different
directions of transport, including east to west, southeast to
northwest and northeast to southwest.  Glaciofluvial deposits are
also geographically widespread on the main claim block and are
dominantly in the form of eskers and related kames.  The eskers
range from small sinuous ridges to large more linear features up to
45 m high, forming the major topographic relief in the area.
The predominant rock type in the Fox area is a medium-grained
biotite granite.  The rock is mostly unaltered but weak to moderate
potassic alteration occurs at the east end of the ravine near the
Fox portal and also along the swamp subparallel to the ravine.  Two
diabase dykes cross the Fox Lake and were identified by an airborne
magnetometer survey and in the decline and confirmed by small
patches of outcrop located to the northeast and south of the lake.
Glacial sediments on the bottom of Fox Lake range from 15 to 25
metres thick and consist of silt and sand-sized particles of quartz,
feldspar, biotite, epidote, amphibole and traces of kimberlite
indicator minerals.  Gravel-sized rock fragments included various
granitoid rocks.  Geophysical surveys and geochemical sampling was
done over the Fox pipe.  In May, 1994 a decline-ramp/underground
mining program was initiated to bulk sample the Fox kimberlite pipe.
When the underground bulk sampling program of the Fox pipe had
been completed, 6,915 tonnes of kimberlite had been extracted.  The
sample yielded 11,960 diamonds weighing 1,766 carats, for and
overall grade of 0.26 carats per dry metric tonne.  The evalusation
of the diamond parce returned an average of US $126.  Underground
raises driven near the pipe periphery to a vertical height of 32
meters and near the pipe center to a height of 32 meters resulted
in higher grade samples of 0.34 and 0.38 carats per dry metric
tonne, respectively.
The Ekati project is held 51% by BHP Diamonds, 29% by Dia Met
Minerals and the remaining 20% is split between Charles Fipke, the
geologist who found diamonds in the NWT and Stewart Blusson,
prospector and partner of Fipke. The mine plan for Ekati involves
the development of the Panda, Misery, Koala, Sable and Fox pipes.
The Fox pipe will be subjected to open-pit mining from years 11 to
17.  Minable reserves are estimated at 16.7 million tonnes grading
0.4 carat at a value of US$125 per carat.  Fox Lake will be
dewatered during the summer before preporduction commences in this
pit, expected to be 2002, the sixth year of project development.
At a pumpling rate of approximately 1,600 cubic metres per hour it
will take four months to pump out the 4.3 million cubic metres of
water contained in the lake.  The turbid water and slimes
encountered as the water level falls will be pumped to a natural
containment area diked off with rock fill in the southern portion
of the old Fox Lake bottom.  Excess water behind this impoundment
will be discharged after solids settling or treatment brings the
water quality below the discharge limits.
The predominant host rock type for the Koala pipe is a white to
grey, medium to coarse-grained, weakly foliated to massive biotite
granite.  The granite locally contains rounded biotite-rich mafic
xenoliths.  A variety of other rock types exist including
granodiorite, granite gneiss and small patches of diorite.  The
granite gneiss, observed about 80 m SE of the lake, contains traces
to 1% almandine garnets that are 1 to 2 mm in size and form
circular pods up to 3.5 cm diameter.  Also within the gneiss are
rare occurrences of tabular tourmaline crystals up to about 2 cm in
length.  The diorite, scattered throughout the area to the east jof
Koala Lake, contains traces of almandine garnet and traces of
disseminated sulphides.  The bottom of Koala Lake and the Koala
kimberlite pipe are covered by unconsolidated sediments of glacial
origin.  This overburden is characterized by a complex
interfingering of sediments lenses ranging from mud to gravel.
Generally the uppermost part of the overburden sequence comprises
well sorted silt and mud.  Elsewhere sand and gravel dominate.  In
most cases, fine clay and silt have been washed and weathered out
of these coarse grained sediments.  Boulders and cobbles are
sporadic throughout the sequence.
It is expected that the Koala pipe will be mined by open pit
methods from years 5 to 11 and by underground methods from years 11
to 15.  Minable pit reserves are estimated at 14.6 million tonnes
grading 0.76 carat, underground reserves at 2.8 million tonnes
grading 1.63 carat.  The diamonds are valued at US$122 per carat.
The Deb volcanogenic massive sulphide deposit is located in the
Courageous - Mackay Lake greenstone belt in the Slave structural
province.  The belt runs north-south, dips steeply to the east and
is composed of Yellowknife Supergroup volcanics.  In the east they
are overlain by Yellowknife Supergroup sediments and in the west
are assimilated from below by granites.  The Deb deposit is
contained within a series of volcanics of varying composition but
seems most closely related to felsic pyroclastics.  Around the
showing sub-volcanic gabbroic intrusions have disrupted the
volcanics.  Massive sulphides are situated within the lower felsic
unit and include massive pyrrhotite, pyrite and sphalerite
underlain by stringers of chalcopyrite and pyrrhotite. The latter
are accompanied by strong chloritization, biotitization,
sericitization and garnets in a small but well-developed alteration
pipe/stringer zone underlying the stratiform mineralization.  The
mineralized horizon is relatively undeformed and has been traced by
drilling over an 800 metre strike length, to a depth of 230 metres
and has an average width of 3.8 metres.  Mineral zonation is
recognizable in both a vertical and lateral sense with respect to
stratigraphy.  Zinc is prominent at the stratigraphic top of the
zone gradually giving way to a copper rich section.  Galena is
generally more abundant within the zinc rich portions.
Drilling in 1979 (assessment report 081299) was successful in
delineating the zone of copper-zinc mineralization.  There were 3
holes drilled in 1980.  One hole tested the gravity anomaly below
the deposit and found it was due to a large gabbro body.  The 2
other holes were drilled to test the deposit at depth.  Core
samples were assayed for gold, silver, copper, lead and zinc.
Results from assaying returned values to 7.21% zinc, 2.76% copper,
2.36 oz/T silver and 1.04% lead.  The 1986-87 Mineral Industry
Report for the Northwest Territories reports that drill testing of
the Deb deposit indicated 1,015,000 t containing 0.83% copper, 2.
96% zinc and 21.9 ppm silver.  The Canadian Mineral Deposits Not
Being Mined in 1989 reports 1,118,000 tons at 0.83% copper, 2.96%
zinc and 0.64 oz/T silver.
The Perrson Vein, BS or TK prospect, is located in the Courageous-
Mackay Lake greenstone belt in the Slave structural province. It is
hosted by a volcanosedimentary sequence belonging to the Archean
Yellowknife Supergroup. The general area of the deposit is
underlain by a stratigraphic sequence including, from oldest to
youngest: mafic flows with minor tuff, mafic tuffs, a mixed unit of
thinly-bedded and alternating mafic and felsic tuffs, felsic tuff
and then clastic sediments. Metamorphic grade at the prospect is
greenschist facies.  Two auriferous zones, the Perrson and East
Perrson zones, occur as seperate stratabound horizons in the felsic
tuff unit immediately below its contact with the overlying
sediments. Mineralization consists of 1 - 3% finely disseminated
pyrite and finely acicular needles of arsenopyrite in a very fine
grained, sericitic felsic tuff with intercalated cherty layers and/
or narrow quartz veins. The Persson horizons vary in width from a
few centimetres to 3 m. Quartz veins and/or cherty layers are
generally conformable to foliation but locally exhibit tight
folding or ptygmatic character.  A third zone, the Saucer Lake Zone,
appears to be hosted by the mixed unit and consists of a horizon
characterized by dark grey to milky quartz veins ranging in width
from 1 cm to 1 m. The veins are variable in orientation, exhibiting
both cross-cutting and conformable relationships and do not contain
sulphides. Arsenopyrite and pyrite occur as clots and crystals in
altered wall rock inclusions in the quartz, the arsenopyrite also
occurring in the wall rocks. In places, the arsenopyrite appears
crudely banded or layered.
Drill logs from the Bow Valley work (AR 082546) describe alteration
in the wall rock as strong chloritization with patches of
hornblende.  The Perrson and East Perrson Zones have been traced by
drilling over lengths of several hundred to one thousand metres and
to a depth of about 125 m. Two drill-hole pierce points somewhat
below a depth of 200 m show that, at least in these areas,
mineralization does not continue to that depth. The Saucer Lake
zone has been traced by drilling over a strike length of about 350
m.  Drilling in 1958 by North Goldcrest Mines Ltd. outlined a
mineralized zone 950 feet in length, averaging 0.51 oz/ton gold
over an average width of 2.2 feet.  The best intersections included
1.54 oz/T gold over 7 feet, 1.48 oz/T gold over 1.3 feet and 0.62
oz/T gold over 2 feet.  In 1983 Roxwell Gold Mines Ltd., using the
1958 drill results, calculated ore reserves for the Perrson Zone to
be 37,500 tons proven and 75,000 tons probable with a weighted
graded average of between 0.13 to 0.15 oz/T gold.  (NMI
076D03AU_06)  The initial gold showings on the BS claims were
discovered in 1945.  Homer Yellowknife Mines conducted limited
diamond drilling in 1947 and 1949 with the first 7 holes testing
the Perrson and East Perrson veins.  All holes encountered gold
mineralization.  The property was subsequently acquired by
Goldcrest Mines Ltd. who conducted some mapping and drilling.  In
1970 the claims were restaked and optioned to Perry River Nickel
Mines in 1974.  The option terminated in 1978.  The claims lapsed
and were restaked and optioned to Roxwell Gold Mines Ltd. in 1981.
In 1983 Giant Yellowknife Mines Ltd. acquired an option on the
property.  In 1987 Bow Valley Industries Ltd. entered an option
agreement with Roxwell Gold Mines.
The Tundra deposit, also known as Fat, is located in the Courageous-
Mackay Lake greenstone belt in the Slave structural province. All
Yellowknife Supergroup and have been metamorphosed to the
greenschist facies.  Two separate gold-bearing zones are present in
a volcanic sequence known as the Matthews Lake Volcanic Complex
which has been divided into a lower and upper cycle. The lower
cycle comprises a 400 metre thick unit of rhyodacitic flows
overlain by 45 - 150 metres of interbedded calcareous sediments and
calcareous rhyodacitic lapilli tuff, and capped by a narrow layer
of locally graphitic pelite. The base of the upper cycle comprises
a 180 - 300 metre thick unit of rhyodacitic lapilli tuff to
agglomerate, overlain by felsic volcanics transitional to typical
Yellowknife Supergroup sediments.  The largest auriferous zone,
known as the Tundra or Fat zone, occurs in felsic volcanics of the
upper cycle. It is a 100 - 250 metre wide zone consisting of
multiple, parallel, subvertically dipping shear zones that are
subparallel to strata. Individual shears range from 3 - 20 metres
in thickness and are characterized by variable but generally strong
sericitization, silicification, chloritization and irregular blue-
grey to dark grey quartz veins and masses. Many of the latter have
diffuse boundaries. Very finely acicular arsenopyrite is the main
sulphide mineral, occurring as disseminations throughout the
sericitized rock and as felted masses. Lesser pyrrhotite and pyrite
occur as disseminations. Chalcopyrite, sphalerite and scheelite
have been identified within the zones but are rare. Gold is largely
refractory, being tied up within arsenopyrite.
However, a significant proportion occurs as free metal in extremely
fine grains averaging less than 10 microns in size. Some of these
occur in fractures or inclusions in arsenopyrite but the majority
is interstitial to silicates. Visible gold is rare and seen only in
some quartz veins.  The Tundra zone has been traced with drilling
over a 1500 metre strike length and locally to a depth of 1300
metres. It is open to depth. A 476 metre vertical shaft was sunk in
1988-89 and 2000 metres of underground development on the 425m
level were completed. In 1989, the Noranda-Hemlo-Total Energold
joint venture announced suspension of the project because of the
relatively low gold grade.  A report prepared by Noranda in 1990
estimates the total geological reserves for the Tundra deposit at
15.47 million metric tonnes grading 6.5 grams per tonne above a 3.4
gram cut-off.  In 1990 a limited surface exploration program was
carried out.  The Carbonate zone is not well described in available
literature. It occurs at the contact between felsic volcanics and
overlying pelites in the lower cycle. It apparently resembles the
Salmita Mine host rock. A reserve of 900,000 tonnes grading 12 g/t
Au is quoted in the 1986-87 DIAND MIR (p265).
The Jax Lake gold deposit is situated within the Courageous-Mackay
Lake greenstone belt in the Slave structural province. All
Yellowknife Supergroup and have been metamorphosed to the lower
greenschist facies except at the north end of Jax Lake, where the
presence of cordierite indicates lower amphibolite facies.
The stratigraphic sequence in the deposit area has been
divided into two cycles. The lower cycle begins with massive mafic
flows successively overlain by banded mafic tuffs, felsic flows and
tuffs, banded mafic tuffs and then graphitic chert. The upper cycle
begins with massive mafic flows, followed by well-banded and
carbonate-rich mafic tuffs, porphyritic massive felsic volcanics
and finally metasediments. Large sills and dykes of metagabbro and
metadiorite tend to occur at the contact between the lower banded
mafic tuffs and overlying mafic flows but are not restricted to
this interval.                      Five auriferous zones have been
identified in a long history of work in this area. The No. 1 zone
strikes northerly, dips vertically or steeply to the east and
consists of a number of light grey to blue-gray quartz veins and
stringer zones at the contact between banded mafic tuffs and
underlying massive flows in the upper cycle. Small amounts (less
than 10%) of sulphide minerals occur in both the veins and adjacent
wall rocks, including arsenopyrite, pyrrhotite, pyrite and lesser
chalcopyrite. Alteration in and around the veins includes epidote,
carbonate and sericite. Inclusions of altered wall rock in the
veins are ubiquitous and some zones contain black tourmaline. Fine
to coarse visible gold is scattered throughout the quartz.
Two main veins about 8 metres apart were traced along a strike
length of about 80 metres. A reserve of 36,300 tonnes grading 14.06
g/t Au has been reported for this zone (VSE SMF for Perry River
Nickel Mines 9/18/80).  The No. 2 zone may be the faulted-off
southern extension of the No. 1 vein and occurs in a similar
geological setting. Gold values are concentrated on the hangingwall
side. Drilling has traced this vein over a strike length of 58
metres and shown it to grade 39.8 g/t Au over an average width of 0.
91 metres.  The No. 3 zone is situated within massive mafic
volcanics stratigraphically below the No. 1 and 2 zones. Three
parallel veins and stringers are present in a 6.5 metre wide zone.
Bluish-gray to black quartz carries up to 5% pyrite, pyrrhotite and
arsenopyrite. Surface samples have returned only trace to low
values of gold.  The No. 4 zone consists of a number of quartz
veins parallelling schistocity that are situated about 60 metres
higher in the stratigraphy than the other zones. Both pyrrhotite
and arsenopyrite are present in the veins, the arsenopyrite also
occurring locally in the wall rock as coarse crystals. Of six
samples collected across 6.5 metres, the best graded 10.6 g/t Au
over 0.7 m. A shallow hole drilled under the outcrop in 1946 cut 2.
5 feet of quartz grading 0.09 oz/ton Au.  A fifth zone is plotted
on a 1960 geology map in AR 017118 and discussed in AR 062023. This
is probably the Sour Lake occurrence which has its own entry in
this database.
The Butterfly deposit is in the Contwoyto-Itchen-Point Sedimentary
Terrane, a large arcuate belt of Archean turbiditic metasediments
belonging to the Yellowknife Supergroup, and affected by polyphase
Archean deformation and regional metamorphism. The sedimentary belt
is flanked to the west by the older, predominantly volcanic Point
Lake supracrustal belt, and invaded to the east and north by late
Archean granitoids. Late Proterozoic diabase dykes cut the
supracrustals and the granites.  The sediments in the showing area
are (garnet-staurolite)-cordierite-quartz-muscovite-biotite schists,
the lower amphibolite grade equivalents of interbedded and graded-
bedded argillites and subordinate greywackes. They are mostly fine-
grained and micaceous, less commonly siliceous, and rarely
graphitic. Cordierite is usually porphyroblastic, rarely incipient
or absent, and often replaced by sericite/muscovite. The cordierite
isograd is well to the west but dips shallowly east under the
deposit. The sillimanite isograd, marking a further rise in grade
to middle amphibolite, is immediately east of the deposit.
Staurolite porphyroblasts are infrequent in the showing area,
andalusite is rare, and garnet occurs near iron formations. Bedding
strikes 120 - 140 degrees and dips 45 - 80 degrees SW in the
deposit area.  Discontinuous lenses and layers of amphibolitic iron
formation are interbedded with the clastic sediments. They are
laminated or crudely banded to massive, with garnet-rich layers,
cherty bands or pyrrhotite defining the layering.
From limited drill data submitted with assessment reports, the
Butterfly deposit is hosted by a discontinuous lens of amphibolitic
iron formation which breaks up along strike into numerous narrow
bands, interdigitating and intergradational with the clastics, and
farther NW along strike becomes a coherent unit of significant
width again. Its strike length is apparently almost 400 m, and it
has been intersected at 60 m depth. Core lengths of auriferous
intersections range from 1 to 5 m. Reserves have been estimated at
100,000 tonnes grading 17 g/t Au, and it is open at depth.  Two
diabase dykes cut the Butterfly iron formation, one trending NW and
the other E.  The dominant schistocity is subparallel to bedding,
and secondary crenulation cleavages are common. Complex folding is
recorded in the compositional banding of the host iron formation.
The showing is in the Contwoyto-Itchen-Point Sedimentary Terrane, a
large arcuate belt of Archean turbiditic metasediments of the
Yellowknife Supergroup, affected by polyphase Archean deformation
and regional metamorphism. It is flanked to the west by the older,
predominantly volcanic Point Lake supracrustal belt, and invaded to
the east and north by late Archean granitoids. Late Proterozoic
diabase dykes cut the supracrustals and the granites.  Little
information is available on the deposit, due primarily to a
conflict over ownership. It is probably a typical Contwoyto-type,
iron formation-hosted gold deposit. The host sediments are
cordierite-quartz-muscovite-biotite schists, the lower amphibolite
grade equivalents of interbedded and graded-bedded argillites and
greywackes. They range from fine-grained and micaceous to siliceous,
and are locally graphitic. They host conformable layers and lenses
of amphibolitic iron formation, commonly banded, and locally
sulphidic with pyrrhotite, pyrite and arsenopyrite being the most
common sulphides. Gold is assocaited with both quartz and sulphides
in the iron formation units across the Lupin area.  From drill hole
locations, limited drill log information, and AEM data, the deposit
is 500 - 1000 m long, 2 - 4 m thick, strikes WNW and dips steeply
north or south. It is probably contorted or folded, as are most of
the iron formation units in the area. It is said to be a
significant deposit (NMI).  A series of granitic sills, probably of
late Archean age, intrude the schists at depth toward the east end
of the deposit horizon (about 1 km E of inferred deposit location
and DDH 88-57); narrow granitic dykes were intersected elsewhere.
A couple of NW-trending diabase dykes probably cut the Jon horizon.
diabase dykes cut the supracrustals and the granites.  The Pan
deposit is hosted by a roughly tabular, NW-striking, moderately NE-
dipping iron formation, enclosed by massive to finely bedded,
foliated metagreywackes with slatey, argillaceous interbeds.
Numerous thin, discontinuous layers of iron formation are
interbedded with the clastics up to 200 m either side of the Pan
horizon. Within a hundred metres south of the deposit the
greywackes grade into more siliceous clastics mapped as siltstones.
A couple of hundred metres west of the deposit, metamorphic grade
rises from upper greenschist to lower amphibolite, marked by the
appearance of cordierite nodules and increasing schistocity in the
sediments. The cordierite isograd runs NW here and dips shallowly
NE.  Intrusion of a 2 x 2 km, late Archean syenitic plug, which
terminates the southern extent of the Pan horizon 60 m SE of the
last drill intersection, caused micaceous hornfels metamorphism of
the sediments and localized intrusive deformation. Two syenite
dykes 2 - 3 m wide strike NE through the Pan horizon. A Helikian
diabase dyke trends NNW about 150 m south of the Pan.
The host unit is a silicate-(sulphide) facies, quartz-garnet-
amphibole iron formation. It is 2 - 6 m thick and auriferous along
180 m. Auriferous intersections 300 m and 780 m on strike to the NW
may derive from the same horizon; exposure is so poor this cannot
be verified. The Pan iron formation is compositionally banded,
hosting Au-poor, garnet- rich layers, and Au-rich, pyrrhotite-rich,
garnet-poor layers, and up to 50% disseminated to semi-massive
arsenopyrite. A 1984 average grade is based on 8 holes, on 40 m
centres testing 20 m and 50 m vertical depths along 183 m, and is 2.
8 g/t Au across an average true width of 3.2 m.
The deposit lies within the Central Volcanic Belt, an E-striking, N-
dipping and -facing sequence of mixed mafic to felsic volcanics
belonging to the Point Lake Formation of the Archean Yellowknife
Supergroup. Two cycles of volcanism have been tentatively suggested
(Bubar and Heslop, 1985). The volcanic belt is bounded to the north
by clastic metasediments of the Yellowknife Supergroup (Itchen and
Contwoyto Formations), and to the south by mixed granitoids, in
part pre-Yellowknife Supergroup basement. Small, late Archean
granitic plutons and pegmatite dykes locally intrude the
supracrustals.  A unit of massive mafic flows with minor
intercalated tuffaceous horizons forms the base of the volcanic
pile. Overlying this is a 500 metre thick sequence of intermediate
to felsic fragmental and volcaniclastic rocks, including the
chloritized tuffs and lapilli tuffs which host the deposit 250 m
above the basal mafic flows. Above the host sequence is a
predominantly felsic volcanic unit, separated from a presumed
second volcanic cycle 2km NW of the deposit by a 1km-wide, fault-
bounded band of metaturbidites.                      The immediate
footwall to the deposit comprises felsic ash and lapilli tuffs,
with minor coarser material and local thin intermediate beds. The
immediate hangingwall is similar but contains a much greater
proportion of coarse felsic volcaniclastics, including matrix-
supported breccias interpreted as debris flows. A thin but
distinctive pyrite-rich, quartz-sericite schist occurs at the
hangingwall contact with the massive sulphides.
The deposit itself is a stratiform, L-shaped body of well-banded,
massive to disseminated sulphides. It lies in the NE-striking,
synformal hinge zone of a regional, open Z-fold, and comprises two
steeply dipping to vertical limbs striking at 170 degrees and 080
degrees.
It is up to 40 m true thickness in the hinge zone, thins rapidly
away from the hinge, but apparently widens with depth along the
north limb where good grades were intersected. Pyrite and
sphalerite are the dominant sulphides, accompanied by variable
amounts of galena and chalcopyrite, and minor amounts of other
metallic minerals. The central portions of the deposit tend to be
enriched in Zn, Ag and Pb while outlying areas are relatively Cu-
rich. Although the deposit is also vertically zoned, with Cu grades
increasing toward the footwall, no significant stringer zone/
alteration pipe has been found to date. The main mineralized zone
in the fold hinge is primarily a Zn-Ag deposit.  Drill-indicated
reserves in 1991 (Northern Miner Dec 09/91) were 7.3 million tonnes
grading 4.8% Zn and 46 g/t Ag, with 0.2% Cu. Up to 2.8 g/t Au is
reported locally.                      Chloritization is the most
wide-spread alteration, comprising chlorite-pyrite ? cordierite ?
garnet, in semi-conformable zones adjacent to the deposit and in
fracture-controlled zones higher up the hangingwall. Sericitization
is less wide-spread and comprises mainly quartz-muscovite-
sericitized feldspar ? pyrite. A third alteration type, chlorite-
cordierite-biotite or CBC, is most distinctive, occurring in
contact with the sulphide mineralization irregularly along both
hangingwall and footwall in zones up to 5 m wide. It comprises
coarse-grained, well-foliated, dark-colored biotite-quartz-chlorite-
cordierite (pyrite-chalcopyrite-sphalerite). A later metasomatic
bleaching, characterized by quartz, K-feldspar and epidote, is
locally superimposed on the above assemblages.
The area has been affected by two folding episodes, the later one
possibly related to shearing and formation of the open Z-fold
hosting the deposit.
Two episodes of brittle deformation, the earlier definitely pre-
pegmatite and possibly coinciding with synvolcanic tectonic
activity and sulphide deposition (Bubar and Heslop, CIMM Bull Apr/
85), have marked the Gondor locality with numerous, steeply dipping
faults. Microfaulting and shearing have been noted in drill core
and on surface. Two regional, NE-striking Proterozoic? faults occur
about 2 km NW of the deposit.
The Hackett River occurrences, also known as the Bathurst
Norsemines occurrences, include a number of volcanogenic massive
sulphide lenses hosted by metavolcanics and metasediments of the
Archean Yellowknife Supergroup in the Hackett River greenstone belt.
Mineralization generally occurs in a mixed package of rhyolitic
fragmentals, epiclastics, chemical and clastic sediments known as
the Mineral Horizon sandwiched between a thick underlying sequence
of fragmental rhyolites and overlying clastic sediments. Three main
areas of mineralization have been described. The Central area
includes the A, Jo and Jo South zones while the Boot Lake and East
Cleaver areas occur at distances of 2 and 6 kilometres respectively.
In the Central area, the A and Jo deposits are situated on a
common stratigraphic horizon and consist of conformable lenses of
pyrite with lesser sphalerite, galena and chalcopyrite. Both
overlie discordant, zoned alteration pipe/stringer zones containing
chalcopyrite, pyrrhotite, pyrite and magnetite. Alteration consists
of a sericite - quartz - (sillimanite - cordierite) assemblage
developed along hydrothermal fluid channelways, interspersed with
patchy anthophyllite - cordierite - biotite - garnet - quartz -
(sillimanite - sericite). Both are contained within a relatively
wide envelope of characteristically spotted sillimanite - biotite -
garnet - quartz - (cordierite - sericite) rock. The Jo South zone
occurs at a lower stratigraphic level and comprises a series of
veins and disseminations of pyrite, sphalerite, chalcopyrite and
galena. The Boot Lake zone also occurs within the Mineral Horizon
although the latter is thinner in this area, with a less complex
internal stratigraphy. Sulphides are present in small lenses and in
continuous layers of pyrite, both containing variable amounts of
pyrrhotite, sphalerite, galena and chalcopyrite.
The East Cleaver zone is a single, fairly homogeneous sulphide body
containing pyrite, sphalerite and galena, also situated within the
Mineral Horizon. It has been deformed through folding and shearing
and is now highly contorted, occupying the nose of an overturned
anticline. Both zones are underlain by a stringer zone/alteration
pipe similar to those under the A and Jo deposits.  A total reserve
for the four zones is reported to be 21 million tons grading 4.98%
Zn, 0.75% Pb, 0.41% Cu, 4.37 oz/ton Ag and 0.013 oz/ton Au
(Northern Miner, 2/21/80).
reasonably continuous in nature. The mineralization is interpreted
open down plunge and along the strike of the limbs (Chandler et al,
The showing is in the predominantly volcanic, north-trending High
Lake supracrustal belt, which in this area is a mixed succession of
Archean Yellowknife Supergroup metavolcanics and metasediments
metamorphosed to lower amphibolite facies, and flanked east and
west by late Archean plutons. A structural history involving
isoclinal folding, at least 3 generations of fabric formation, and
late faulting, is not yet unravelled.                      The
geology below is largely derived from Flood (1991).
The Ulu area is a lobe of supracrustal rocks on the west
margin of the High Lake belt. It is separated from the main part of
the belt by a narrow granitic apophysis. The supracrustals comprise
a sequence of basalts, greywackes and gabbroic sills, all folded
into a 5 km-long, doubly-plunging? anticline. Later Archean
feldspar-porphyry and quartz- diorite dykes and Proterozoic diabase
dykes transect this sequence.                      Auriferous zones
are near the axis of the north-trending anticline. The largest zone,
the Flood Zone, strikes NW and dips steeply for 400 m on the west
limb of the anticline, near the sediment-filled core. The main part
of the zone is 2 - 5 m thick, increasing to 10 m at points of
flexure along the roughly tabular body, and has been intersected at
depths over 600 m. Lesser developed, en echelon hangingwall and
footwall zones have also been recognized as part of the Flood Zone.
Structural features of note include brecciation and re-brecciation,
vein paragneiss, and local mineral segregation in shear banding.
These point to multiphase brittle and ductile deformation.
Auriferous zones comprise intense silicification and
acicular arsenopyrite development to 5%; arsenopyrite occurs as
needle aggregates within veins and fractures and as complete
replacement of basalt breccia fragments.
Gold occurs mainly at quartz-arsenopyrite boundaries. Pyrrhotite,
pyrite and minor chalcopyrite are present as well as a variety of
alteration minerals (see Mineralization section). An alteration
envelope comprising a stockwork of quartz-actinolite veins and
biotite-microcline enrichment extends 2 - 5 m from the ore zone.
This is consistent with the K-enrichment and Na-depletion
characteristic of Archean hydrothermal systems.
Quartz-actinolite veins within the Flood Zone strike more
northerly than the zone itself, which is approximately
perpendicular to the regional foliation (S3), suggesting a left-
stepping en echelon array (Henderson 1993).
Reserves are guesstimated by DIAND geologists at over 1 million
tonnes of greater than 10 g/t Au.
The Gumbo Lake Ilmenite deposit is hosted by a late Archean or
early Proterozoic mafic complex, intrusive into Archean Yellowknife
Supergroup metavolcanics of the Kathawachaga (Southern) segment of
the High Lake supracrustal belt. This segment trends NE and is cut
off from the High Lake belt proper by, and surrounded by,
batholithic intrusions of late Archean granitoids. It has undergone
polyphase Archean deformation, and metamorphism to greenschist
facies.                      The host mafic complex intruded NE to
north striking, moderately to steeply west dipping massive basalts
and tuffaceous dacites at the extreme northeast end of the
Kathawachaga segment. The gabbro-norite and leuconorite complex is
elongated NNE and shallowly dipping.                      A roughly
circular, more mafic component of the complex, near its centre,
comprises noritic metagabbro. This varies from meso to leucocratic,
and from diabasic to porphyritic and cumulate-textured. Ilmenite in
this central mafic part of the complex is ubiquitous as an
accessory, and in two significant pods varies from 10% to 70% of
the rock. The Eastern and Western pods, 400 m apart, were gridded
and sampled at 7.6 m intervals, but roughly half the 105 samples
were destroyed by fire before assaying, leaving 34 from the Eastern
grid and only 8 from the Western. From these a rough approximation
of tonnage was arrived at for the Eastern zone (AR 080184), with
grades somehow higher than any of the component sample assays: 252,
000 square ft (61,550 tons/vertical ft) at 18.42% Fe, 0.22% V and
11.86% Ti. The surface expression of the pod is approximately 600 m
long in a northerly direction and 100 m across, though
Its grade is estimated to be at least equal to that of the Eastern
pod; 3 samples along 15.2 m averaged 15.50% Fe, 0.16% V and 9.60%
Ti.                      Numerous granitic dykes intrude the
complex.                      Roscoe (GSC Paper 1985-1A) suggests
the complex is part of the Booth River Intrusive Suite, a layered
mafic/ultramafic complex 60 km to the east, intruded after Archean
granitoids and before Aphebian Goulburn Group sediments.
The Anialik River Intrusive Complex hosts the North Vein, which
includes the North Central Vein deposit at its northeast end and
the North Vein South Zone showing at its southwest end, as well as
numerous other auriferous, shear-hosted quartz veins collectively
known as the Arcadia or Coronation Gulf showings. Relief in the
area is approximately 60 m, exposure about 50%.  The complex is an
elliptical, NNE-trending, 35 by 15 km pluton whose gold showings
are concentrated in the northwest portion. Its dominant phase is a
variably deformed and altered leucotonalite with subordinate
trondhjemite. Locally intermixed mesotonalite forms a variety of
migmatitic textures. Such rocks host most of the North Vein system,
including North Central Vein. Mafic phases and intensity of
deformation in the pluton increase toward its margins, so that a
margin-parallel band of mesotonalite hosts the southwest end of the
North Vein system, and grades west into the mafic marginal phase
(Abraham 1989), a heterogeneously deformed band of foliated,
sheared or migmatitic diorite, mesotonalite, and gabbro. The actual
contact of the pluton with supracrustals, approximately 1km west of
North Central Vein, is the sheeted zone of Abraham, a 200 - 800 m
wide shear zone comprising mylonitized equivalents of: plutonic
rocks; metavolcanics; and numerous, foliation-parallel,
Recent dates from the volcanic belt give roughly the same span of
activity yielded by the tonalites, minus the oldest date
(Villeneuve 1992 dates referred to by C.Relf, Geoscience Forum,
DIAND Yellowknife 1992).  The pluton is cut by at least five
generations of dykes: sheared, boudinaged and chloritized gabbro
dykes; later (syn-intrusion?) intermediate dykes; and three sets of
felsic dykes distinguished by orientation. Two of the felsic sets
are sheared, boudinaged, folded and locally mylonitized, and may
have been loci for development of shear zones; they are locally
mineralized where they occur in auriferous shears (eg. North
Central Vein). The third set of felsic dykes commonly cross-cuts
the other two but locally is cross-cut by them, and never cross-
cuts mineralized shears. All are regarded as pre to syn-shearing.
Syn to post-tectonic granitoid plutons intrude the complex and the
surrounding volcanics 6 km southwest and 2 km northwest of the
deposit. Late Proterozoic diabase dykes trend northwest throughout
the area, and Proterozoic gabbro sills cap the Archean rocks
approximately 3.5 km north of the deposit.  The pluton records two
phases of Archean deformation (Abraham 1989, 1990, 1991) although
three are recognized in the surrounding supracrustals (Relf 1992).
D1 apparently coincided with diapir emplacement and generated a
margin-parallel foliation throughout the complex and some isoclinal
folding in the western portion. Metamorphism of the surrounding
volcanics to amphibolite grade and development in them of a margin-
parallel S1, also took place at this time.
D2 is thought by Abraham to have been a regional translational
shearing event. It produced a mild to intense, northerly to
northeasterly fabric in the complex, as well as discrete zones of
mylonitization including four major shears and dozens of minor ones.
All the mineralized shears are thought to be D2. Most of them
strike NE but some strike NNW.  The last deformation was
Proterozoic east to west, dextral and sinistral faulting which
offset Archean fabrics and late diabase dykes.  North Central Vein
belongs to the North Vein system, which is exposed intermittently
in anastomosing shears for 5.5 km. The North Central Vein is
thought to have developed by fracture-controlled, multiple-stage
quartz injections. It consists of quartz stringers, pods and lenses,
and locally of quartz matrix to a breccia of mylonitic wall-rock
fragments. The North Central Vein strikes northeast for 700 m and
is approximately 1.5 m wide. Gold mineralization is found within
the quartz, and within cross-cutting, mylonitized felsic dykes.
Quartz was apparently injected in three stages, the first two late
in the D2 event (Abraham). Gold has so far been identified in the
first stage only, associated with highly deformed pyrite. The
second stage relates to extensive hydrofracturing and euhedral
pyrite. The third consists of post-tectonic quartz-(carbonate) in-
filling and often contains specular hematite.  The age of the syn-
shearing mineralization is bounded by the youngest tonalite age
(2682 +/- 2Ma) and the age of the post-tectonic Chin Lake Stock, 6
km SW of the deposit (2602 +/- 2Ma). A hydrothermal alteration
event at 2670Ma is recorded in titanite from the North Central Vein
hanging wall; this may be related to the mineralizing event
(Abraham 1990).
Excitement over the North Central Vein was generated in the 1960s
when 320 feet at its south end was opened by 10 trenches averaging
0.84 oz/ton Au across 5 ft, four trenches along 160 ft in the
middle averaged 0.48 oz/ton across 4 ft, and 26 trenches along 1200
ft at the north end averaged 0.33 oz/ton across 5 ft. By 1987, the
Vein had been tested by 74 trenches, over 150 drill holes and three
bulk samples. Reserves of 160,772 tons of 0.353 oz/ton Au proven,
probable and possible, and of 737,000 tons of 0.205 oz/ton Au
proven and probable, have been outlined using different methods
with the same data (see Reserves section of this report).  The No.
11 Vein of 1965 is just northeast of the 1965 North Vein, perhaps
part of the same system. It returned trench sample assays averaging
13.03 g/t Au across 1.4 m and 60 g/t across 0.9 m. Its relationship
to the current North Central Vein is uncertain; it is definitely
nearby and may be regarded as part of it.
The Anialik River Intrusive Complex hosts the Fred Vein deposit and
foliated to gneissic leucotonalite with subordinate trondhjemite.
Locally intermixed mesotonalite forms a variety of migmatitic
textures. Such rocks host the Fred Vein. Mafic phases and intensity
of deformation in the pluton increase toward its margins, through a
margin-parallel band of mesotonalite to a heterogeneously deformed
band of foliated, sheared or migmatitic diorite, mesotonalite, and
gabbro (the mafic marginal phase of Abraham 1989). The actual
contact of the pluton with supracrustals, approximately 1.5 to 2 km
west of Fred, is the sheeted zone of Abraham, a 200 to 800 m wide
shear zone comprising mylonitized equivalents of plutonic rocks,
metavolcanics, and foliation-parallel felsic dykes.  The complex is
covered in the north by water. It is surrounded on all other sides
by predominantly felsic metavolcanics of the Anialik River volcano-
(sedimentary) belt, and is thought by Abraham (1990, 1991) to be
largely coeval with them and emplaced diapirically into them. (For
age dating, see the North Central Vein entry in this database.) It
is cut by a set of altered mafic dykes, another of intermediate
dykes, and three sets of felsic dykes. All are pre to syn-shearing.
Syn to post-tectonic granitoid plutons intrude the complex, and the
surrounding volcanics, 8 km southwest and 3 km northwest of the
deposit. Late Proterozoic diabase dykes trend northwest, and
Proterozoic gabbro sills cap the Archean rocks approximately 3.5 km
north of the deposit.  The pluton records two phases of Archean
deformation (Abraham 1989, 1990, 1991) and one of Proterozoic
faulting (for more detail see North Central Vein). All the
mineralized shears are thought to be D2. Most of them strike NE but
some strike NNW. Quartz injection and gold mineralization took
place late in D2.  The Fred Vein is roughly 250 m long. Its
relationship to the Pick and Northwest Veins of 1965 is uncertain
but it is probably nearby. Pick was opened in 13 trenches which ran
from 2.74 g/t Au across 0.3 m to 30.86 g/t across 1.22 m. Northwest
Vein yielded a grab of 78.17 g/t and a best chip of 26.06 g/t
across 0.5 m. In the Fred Vein, reserves of 38,338 tons of 0.44 oz/
ton Au proven, probable and possible, and of 101,000 tons of 0.25
oz/ton Au proven and probable, have been outlined using different
methods with the same data (see Reserves section of this report).
The High Lake AB Zone is within the north-trending High Lake
supracrustal belt, which comprises mainly Archean Yellowknife
Supergroup metavolcanics.  The High Lake deposits are hosted by a
200 m wide unit of altered and sheared, felsic and intermediate
pyroclastics, consisting of fragments of dacite and siliceous
rhyolite in an andesitic to dacitic matrix.  A rhyolitic flow and
narrow bands or lenses of carbonate-cemented, felsic breccia are
interbedded with the pyroclastics of this unit, east of the
deposits. This unit is part of a north-striking, steeply dipping
succession, and is underlain to the east by massive, pillowed and
tuffaceous andesites and dacites, and overlain to the northwest by
rhyolite or rhyodacite tuffs.  The AB Zone, approximately 600 m
north of the D Zone (separate report in this database), is a series
of subconformable, Cu-rich, stringer-dominated sulphide lenses,
striking northeast and plunging north, within intensely altered
rocks (see Mineralogy). The zone measures maybe 150 by 75 by 75 m;
it is exposed on surface as two discontinuous, NE-trending gossans,
These range from hornblende-hornfels metamorphism and
recrystallization, to the development of dalmatianite in the
already-altered ore host (see Mineralogy).  A younger, late Archean,
granitic batholith is exposed approximately 3km east of the
deposit.  Deformational history involving at least two phases of
Archean folding is obscured by intense northerly shearing and
common northwesterly faulting. The AB Zone itself is sheared and
cut by faults. A 1 m wide, late Proterozoic diabase dyke cuts north
through the deposit area, and a 10 m wide one follows a NW-trending
fault through both the AB and D Zones, offsetting the latter by
about 40 m dextrally. The Kennarctic River, 1 km east of the
deposit, traces a regional, north-trending shear zone.
The High Lake D Zone is within the north-trending High Lake
rhyolite or rhyodacite tuffs.  The D Zone polymetallic deposit,
approximately 600 m south of the AB deposit, is a NE-striking, W-
dipping, 100 m long by 100 m deep zone, ranging from 18 m thick
near surface to 60 m at depth. It comprises mainly finely
disseminated, and locally stringer and banded, sulphides within
intensely altered rocks (see Mineralogy). The E zone, 180 m east of
D Zone, and the C zone, approximately 300 m north of D Zone, are
included here with the D Zone. They have generally
recrystallization to the development of dalmatianite in the already-
altered ore host (see Mineralogy).  A younger, late Archean,
granitic batholith is exposed approximately 3 km east of the
common northwesterly faulting. The D Zone itself is sheared and
faulted. A 1 m wide, late Proterozoic diabase dyke cuts north
The Pistol Lake iron formation-hosted gold deposit is located in a
supracrustal basin in the northern part of the Slave structural
province. All stratified rocks have been metamorphosed to lower
amphibolite facies. Significant gold mineralization is present in
two iron formations (IFs) situated within a tightly folded and
overturned sequence of medium grade turbiditic sediments dipping
west at about 40 degrees. Host turbidites are distal in character,
exhibiting A(D)E divisions of the Bouma sequence. The older iron
formation is silicate facies and hosts the F and Farney auriferous
zones while the younger is oxide facies and hosts the G Zone. The
iron formations are separated by about 225 metres of metasediment.
No metavolcanic rocks are present in the immediate area. A late
granitoid intrusive cuts the sequence about 2 km north of the gold
occurrences. The silicate iron formation is up to 10 metres thick
and is banded on a number of scales, from mm sized laminae of
amphibole, chert and biotite-garnet schist to decimetre scale
intercalations of iron formation with clastic sediments.
Significant levels of gold occur in highly siliceous iron formation
where it is deformed into 50 - 150 metre scale folds. Away from
these folds, the iron formation decreases both in thickness, silica
content and the number of included amphibolitic bands. Sulphide
minerals include pyrrhotite and arsenopyrite, the latter commonly
containing cores of loellingite. Pyrrhotite occurs most commonly in
fine grained laminae while arsenopyrite usually forms larger
subhedral to euhedral crystals, often scattered along pyrrhotitic
laminae and in aggregates in the vicinity of cross-cutting quartz
veins. Gold occurs as 5 - 100 micron grains in arsenopyrite,
frequently at the boundary between that mineral and its loellingite
core.
The oxide iron formation is composite in that it consists of a
series of stacked facies types with an aggregate thickness on the
order of 50 metres. A basal horizon of silicate IF is successively
overlain by finely laminated oxide IF, silicate IF, graphitic chert
and a series of decimetre scale intercalated amphibolite and
clastic metasedimentary beds. Significant levels of gold occur in
the G Zone, situated at the base of the laminated oxide IF unit
where stratabound arsenopyrite-pyrrhotite mineralization is
associated with irregular quartz veins and masses along with
recrystallized silicate minerals. Recrystallized areas commonly
exhibit disrupted and brecciated textures, with variably
mineralized fragments in a matrix of silicate and sulphide minerals.
Two main types of sulphide distribution exist. The most important
in terms of gold content is characterized by ragged blebs and
coarse disseminations of pyrrhotite occurring in recrystallized
areas proximal to quartz veins. Arsenopyrite is almost always
present and occurs as subhedral crystals and crystal aggregates. It
often contains inclusions of pyrrhotite and cores of loellingite.
Gold is found as grains up to 100 microns across in arsenopyrite,
often at the boundary with loellingite, and as larger grains up to
2 mm across in the silicate matrix. Visible gold is commonly
observed in drill core. The second type of mineralization preserves
the morphology of laminated oxide IF except that magnetite is
replaced to a variable extent by pyrrhotite. Where replacement is
extensive, crystals of arsenopyrite are scattered along pyrrhotite-
rich bands. Gold is present in the former as grains up to 10
microns across.
Numerous trenches were opened and sampled, and a total of about 11,
080 metres in 66 diamond drill holes were drilled, mainly in the F,
G and Farney zones (Farney is covered in a separate report),
between 1964 and 1988. A small amount of this information is
published in Assessment Reports, including such F Zone
intersections as 34 g/t Au over 3.0 m and 36 g/t over 1.5 m in hole
PL-1, and 7.9 g/t over 1.5 m, 12.5 g/t over 3.0 m and 3.8 g/t over
1.5 m in PL-2, and trench samples of 18.5 g/t Au across 0.9 m from
F Zone and 27.4 g/t across 0.6 m in G Zone. Most of the results,
however, are not public. Reserves in the northern part of F Zone
were estimated in 1984 at 218,337 indicated tonnes averaging 14.78
g/t Au, and reserves in F and G Zones combined were estimated in
1985 at 489,880 tonnes at 13.92 g/t Au (Silver Hart Mines Letter to
Shareholders).
The Turner Lake area lies in the NE corner of the Slave Province,
just west of Bathurst Inlet, toward the north end of the Hood River
Sedimentary Belt. This belt is a roughly H-shaped, NE-trending area
underlain by Archean Yellowknife Supergroup clastic sediments and
minor volcanics, locally intruded by pre-metamorphic amphibolitic
bodies. It has been affected by at least two phases of Archean
deformation, metamorphosed up to middle amphibolite facies, and is
flanked and locally invaded by late Archean granitic rocks. It is
cut off at its NE end by the Bathurst Fault, which has juxtaposed
Aphebian Goulburn Group sediments, to the east, against the Archean
rocks, to the west. Late Proterozoic gabbro sills and diabase dykes
intrude all other lithologies.  The Turner Lake area is
characterized by 30 - 130 m relief and approximately 60% outcrop,
ranging from extensive in uplands to none in valleys (AR 082608).
The deposit itself is poorly exposed. It lies about 800 m west of
Turner Lake, in an area underlain mainly by turbiditic greywackes
and minor argillites in a steeply dipping, E-facing, N-striking
homoclinal succession. Interbedded with or conformably intruding
the sediments are beds of polymict, clast-supported conglomerate,
metadiorite synvolcanic? sills, banded amphibolitic rocks, and the
host mineralized amphibole-plagioclase schist, all belonging to the
Yellowknife Supergroup, and sheets of granodiorite of later Archean
age. Pods of pegmatite cross-cutting these lithologies are probably
related to the undeformed, late Archean granitic batholith exposed
2.5 km west of the deposit. A plug of undeformed but metamorphosed,
Proterozoic? (Schaan 1992) olivine gabbro intrudes the sediments 2.
4 km south of the deposit and hosts significant Ni mineralization
(the Nickel Knob showing).
NW-trending diabase and gabbro dykes and sills of at least 2
Proterozoic generations are exposed near the deposit as well.
The high degree of deformation and alteration within
the older Archean rocks has hampered determination of protoliths. A
N to NNE-striking, braided shear zone transects the region, leaving
rocks within and to either side of it with a pronounced shear
fabric. 300 m to 1000 m scale drag folds are well developed on the
east side of the shear. The Turner Lake Main Gold deposit lies in
the nose and on the north limb of one such 300 m wide, E-closing
fold.                      The fold is defined primarily by a
banded (feldspar?) chlorite? biotite-amphibole schist or gneiss,
perhaps an altered mafic or ultramafic intrusive or mafic extrusive
(see Comments under Host Lithology). The structure plunges almost
vertically, closing to the east about a steeply dipping, E-W axial
plane. The north and south limbs form an angle of approximately 60
degrees and dip steeply south and north, respectively. Metadiorite
lies in the core of the fold, and metasediments surround it, along
with a metadiorite
Gold is associated with sulphides, which are associated with quartz
veining. The principal sulphides are pyrrhotite, which is
disseminated throughout the quartz-veined rock, and arsenopyrite,
which is concentrated in and around the quartz veins themselves.
The quartz veins are of more than one generation, and some are
marked by hornblende - cordierite - sillimanite? garnet selvages
which may be hydrothermal alteration assemblages further altered by
regional metamorphism (Clode 1987). The best gold tenors are in the
nose of the fold and in the noseward portion of the north limb.  A
regional foliation strikes NE and dips steeply NW (AR 082608).
Movement on the major N to NNE shear was sinistral, and localized E-
W folds with associated axial planar foliations, such as hosts the
Main Gold deposit, may have formed as drag folds during the
shearing event (AR 082608, Clode 1987, Schaan 1990).  Metamorphic
grade is middle amphibolite, except within the shear zone where
upper amphibolite conditions and incipient melting have produced a
sillimanite - cordierite - microcline gneiss from a granodioritic
or pelitic protolith (Clode, 1987, AR 082608).  Based on earlier
subdivisions (eg. AR 017152), the deposit is here described in 3
zones and a fourth sample location: the easternmost Nose zone
(weighted average chip samples including 8.42 g/t Au across 13.7 m),
NC (north-central) zone approximately 250 m WNW of Nose (chips
including 11.17 g/t across 5.4 m), NW (northwest) zone
approximately 400 m WNW of Nose (chips including 17.76 g/t Au
across 1.8 m), and W (west) location approximately 600 m WNW of
Nose, which yielded anomalous grabs (5 and 18 g/t) apparently from
float transported from the other zones.
Reported DDH intersections tend to be lower grade, except some
recent holes (Silver Hart Annual Report 1987) which cut such
intersections as 8.9m grading 12.86 g/t. A 1987 reserve estimate
based on 17 widely-spaced DDH and chip and panel chip samples from
47 trenches, mostly in and near the Nose zone, is 1.18 million
tonnes grading 5.35 g/t Au.
Boston is a gold-bearing shear zone located in the southern portion
of the Hope Bay Greenstone Belt.  The Belt is composed of volcanic
and sedimentary rocks of Archean aged.  The shear has a strike
length of approximately 70 kilometres.    The mineralized shear was
first dicovered in 1988 by Abermin Corporation who outlined 9
kilometres of intense quartz-carbonate shearing.  Government
geologists from RWED and DIAND provided follow up mapping of the
area.  The Boston claims were staked in 1991 by BHP Minerals Canada
Ltd. and exploration on the property commensed sortly afterwards.
By 1997 an underground ramp was developed into the shear zone and
over 50,700 metres of coring was completed.  A resource calculation
was also preformed on Boston resulting in figures of  2 to 3
million ounces of gold (reference RWED RWED, MOG Book (1997)).
The various mineralized zones comprising the Great Slave Reef
Mississippi Valley type Pb-Zn deposits are located in the Pine
Point Pb-Zn district immediately south of Great Slave Lake.
Mineralization occurs in a large, middle Devonian barrier reef
complex separating two depositional basins in the Interior Platform,
the northern Mackenzie shale-carbonate basin and the southern Elk
Point evaporite-carbonate basin. The reef complex consists of a
lower Pine Point Formation buildup of skeletal-derived carbonate
sands and muds, and an upper Sulphur Point Formation buildup of
biohermal to bioclastic limestone.  Most of the Pine Point district
Pb-Zn mineralization was deposited in interconnected paleokarst
networks that developed at the lower limits of coarse dolomite
alteration (known as Presquile dolomite) within the Sulphur Point
limestones. The karst networks are present in two main zones known
as the North and Main trends. Sphalerite, galena, pyrite and
marcasite occur as replacements and open-space fillings within
karst openings and in vuggy wall-rock peripheral to the karst
openings.  The Great Slave Reef deposits are situated immediately
west of the Pine Point property at depths between 150 and 300 m.
Grid drilling resulted in the discovery of four deposits. Two more
were discovered through followup work on IP anomalies and one
deposit was found on the basis of geological and trace element data.
By the end of 1981, a total of seven deposits containing an
aggregate tonnage of 7.25 million tonnes grading 10.3% combined Pb
and Zn had been outlined.
The XL base metal massive sulphide prospect is located in the
Turnback Lake area. It lies in the Beaulieu Volcanic Belt, a
supracrustal belt in the Archean Slave structural province.
Volcanism in this portion of the greenstone belt commenced with the
eruption of the tholeiitic Tumpline Basalt and concluded with an
approximately equal volume of felsic volcanics referred to as the
Turnback Rhyolite. Metaturbidites of the Burwash Formation overlie
the Turnback Rhyolite. A carbonate exhalite unit is commonly
developed at the contact between them. Volcanics and sediments, all
part of the Yellowknife Supergroup, are metamorphosed to
amphibolite facies. Stratified rocks are strongly deformed around
the Sleepy Dragon Complex.  The XL prospect was discovered in 1937
by prospectors Lars Johnson and Garfield Smith, and was optioned by
Westfield Mining Company Ltd. in 1938. Westfield drilled 14 holes
totalling 2450 ft, excavated 15 trenches, completed geological
mapping at a scale of 1:480 and conducted a dip needle survey. No
direct record of this work exists and the desciption below, as well
as the description of mineralization, is taken from summaries by W.
M. Little in AR 017321 and C.S. Lord in GSC Memoir 261.
Mineralization tends to occur within the Burwash Formation along or
near the contact between it and the Turnback Rhyolite, in places
within the carbonate exhalite between them. It has been divided
into four zones, the A, B, C and N. These appear to lie within a 40
m thick stratigraphic interval over a total strike of about 600 m
but are separated by intervals of relatively weak mineralization.
In parts of the 40 m interval, only one sulphidic band is present,
while in other parts, four or more occur over the 40 m.
Massive and disseminated pyrrhotite, sphalerite, chalcopyrite,
galena and pyrite are present (in that order of abundance). The N
zone occurs in amphibolite and differs somewhat in that it consists
of a large number of discontinuous stringers and fine
disseminations of chalcopyrite, along with about 1% pyrrhotite as
fine disseminations. Very minor sphalerite and a few specks of
native copper are also present. AR 082901 notes the abundant
development of a needle-like amphibole in the vicinity of the XL
deposit and the OK deposit to the southwest. This is tentatively
interpreted as the metamorphic derivative of hydrothermal
alteration in the enclosing rocks.  AR 017321 estimates a reserve
of 910 tons per vertical foot at a grade of 6% Zn, 2% Cu, 1.5% Pb
and 3 oz/ton Ag. Apparently, drilling by Westfield suggested that
mineralization was cut off by granite at a depth of about 200 feet
at the A zone and would probably be truncated above a 500 foot
depth elsewhere. AR 082654 restates the reserve figure as an
aggregate reserve of 180,000 tons at the same grades and to a depth
of 90 m.
The Sunrise volcanogenic massive sulphide deposit occurs in the
Beaulieu River supracrustal belt, a predominantly volcanic belt in
the Archean Slave structural province. All stratified rocks in the
belt belong to the Yellowknife Supergroup, the volcanics in the
Sunset Lake area belonging to the Beaulieu Group. The stratigraphic
sequence forming the footwall of the deposit begins with a
rhyolitic lapilli tuff to agglomerate known as the Western Rhyolite,
and continues upward with tuffaceous argillite, sericitic felsic
tuff and rhyolitic pyroclastic breccia. Sulphide mineralization
occurs at the contact of the pyroclastic breccia with an overlying,
sericitized and occasionally chloritized, fine grained felsic tuff.
Immediately overlying these mineralized and altered units is a
mafic package including intermediate to mafic pillowed flows and
lapilli tuffs. This is in turn overlain by a felsic package
including sericitized quartz eye rhyolitic tuff, argillite,
intermediate flows and felsic fragmentals, and then by a thick
package of intermediate to mafic flows. The sequence generally
strikes northnorthwesterly and dips to the east at 65 - 80 degrees.
A sinistral NE fault, named the Campsite Fault, has offset
stratigraphy by about 1400 metres. The Bear massive sulphide
deposit owned by Silver Hart Mines Ltd. across the fault appears to
be at the same stratigraphic level as the Sunrise deposit.
Sulphide mineralization includes pyrite, sphalerite and
galena with lesser tetrahedrite, arsenopyrite, pyrrhotite and
chalcopyrite. Other metallic minerals identified to date include
pyrargyrite, boulangerite, native silver, native gold, gudmundite
and stannite. The base of the sulphidic sequence is constituted by
a layer of semi-massive sulphides which is actually a strongly
brecciated rhyolite with a sulphide matrix.
The main sulphide lens includes very well banded, fine to medium
grained material together with massive, coarse grained sulphides,
the latter being brecciated in places. Coarse lithic fragments
within the sulphide horizon suggests proximity to a vent.
Footwall stringer mineralization is described only as
minor stringers of sphalerite and galena, patchy pyrite and minor
chalcopyrite accompanied by silicification. The discovery outcrop
consists of this stringer style mineralization and a sample
returned a value of 35 g Au/tonne. A limited lithogeochemical study
suggests strong Na2O depletion.  The deposit has been outlined by
65 diamond drill holes which show a strike extent of 160 metres and
an average thickness of 3 - 4 metres. It has been traced down dip
for 700 metres and is open to depth. A steep northerly plunge of
about 65 degrees is evident in longitudinal section. Reserves are
estimated at over two million tonnes grading 8.88% Zn, 4.22% Pb,
and 400 g/t Ag (Aber Interim Rpt, 10/31/88).
The Bear or M-zone volcanogenic massive sulphide deposit occurs in
the Beaulieu River greenstone belt, a supracrustal belt in the
Archean Slave structural province. All stratified rocks belong to
the Yellowknife Supergroup, the volcanics in the Sunset Lake area
belonging to the Beaulieu Group. Stratified rocks are intruded by
late Archean gabbro and granite as well as Proterozoic diabase
dykes. Massive sulphides are hosted by an east facing,
northwesterly trending and easterly dipping sequence of volcanic
and sedimentary rocks.  The base of the sequence in the immediate
vicinity of the deposit is constituted by a series of pillowed to
massive andesites to basalts. Thin units of fragmentals and
interflow sediments are present in places within this unit. Several
kilometres to the north and to the west, this unit includes oxide
iron formation. Overlying the mafic package is a unit of quartz
feldspar porphyritic rhyolite flows and fragmentals, part of which
appears to form a small endogenous dome. Alteration in the form of
kaolinitization, sericitization and silicification is present. The
rhyolites are in turn overlain by a sequence of mixed greywacke,
chert, graphitic argillite and mafic to felsic tuff. M zone massive
sulphides occur as two separate horizons at this point, a lower
silver-rich, narrow (2 m) zone sandwiched between a graphitic
argillite beneath and a carbonate-rich exhalite above, and a
thicker (15 m) zone in an overlying unit of rhyolitic tuff to
coarse pyroclastics. The mineralized horizons are successively
overlain by pillowed to fragmental mafic volcanics, intermediate
fragmentals and flows, and then argillite. A thick quartz feldspar
porphyry sill occupies the contact between the mafic and
intermediate units.
The lower mineralized zone is generally less than 2 metres thick
and consists of a base of laminated pyritic argillite grading
upward into semi-massive pyrite with minor base metals and then
into variably bedded massive sphalerite, galena, pyrite and
sternbergite. A thin (20 cm), greenish and pasty band of sphalerite,
sternbergite, marcasite, galena and other silver minerals overlies
the massive sulphides. This lower zone is separated from the upper
mineralized zone by a unit of felsic fragments, carbonate, minor
argillaceous material and variable amounts of sulphides together
with tuffaceous greywacke.  The upper mineralized zone consists of
a base of semi-massive to massive pyrite successively overlain by
massive pyrite with variable but minor base metal sulphides, and
semi-massive to banded sphalerite and galena with only limited
amounts of pyrite. A third and minor sulphide horizon with a
sulphidic argillite base is seperated from the upper mineralized
zone by a debris flow.  Drilling has traced the M zone horizons
over a strike length of 160 metres and to a depth of about 400
metres. Longitudinal sections show a north northeasterly plunge of
about 70 degrees for the deposit, which is open to depth.
Mineralization (massive to disseminated pyrrhotite, sphalerite,
chalcopyrite, pyrite, galena, some silver and molybdenite) forms
long narrow conductive zones parallel to the bedding of Archean
Yellowknife Supergroup metasediments that define a broad east
plunging syncline. Two zones  make up the Turnback Lake showing,
the XL zone and the OK zone. The XL zone consists of two en echelon
lenses that are 1900 feet long and terminated bynpegmatite and
granite.   Work done on this showing includes geological mapping,
geochemical sampling, magnetic (ground?) and EM surveys (airborne
and ground), trenching and diamond drilling. Resources calculated
for the XL zone are listed as diamond drill inferrred at 2,000 ton/
vertical foot at 4 oz/T Ag, 0.8% Cu, 4.7% Zn and 1% Pb. The OK zone
is reported as being 30x5.3 feet in extent at 18.8 oz/t Ag, 8.4% Pb
and 13.7% zinc.
The KI pegmatite dyke swarm occurs in the Yellowknife
metasedimentary basin within the Slave structural province. It is a
member of the Yellowknife pegmatite field, a series of pegmatites
east of Yellowknife, NWT that are probably associated with a number
of late Archean granitoid intrusions of the Prosperous Granite
suite. The pegmatites tend to occur in Burwash Formation sediments
where those have been metamorphosed to lower amphibolite facies.
The pegmatites show a broad zonation around the larger intrusives
in the area; an inner zone dominated by Be-rich pegmatites is
successively enclosed by zones dominated by Cb-Ta-rich varieties
and then by Li-rich varieties.  The KI dyke is of the Li-rich
variety. It strikes at about 135 degrees and dips steeply to the
southeast. It can be traced on surface for about 800 m and is 10 -
15 m thick. There is no marked zonation and the dyke is classified
as a simple pegmatite, consisting of 20 - 25% spodumene as 15 cm
pale green crystals and, in decreasing order, microcline, quartz
and muscovite. The spodumene crystals are generally oriented
perpendicular to the strike of the dyke. Hornfelsed wallrock
inclusions are common in the southern portion. Drill logs note the
development of secondary alteration comprising a fine-grained,
aplitic mixture of sericite, albite and hematite.  A reserve of 2
million tons grading 1.4% Li2O based on surface sampling and
geological projection to a depth of 500 feet is estimated in AR
080274. One bulk sample taken in 1987 (AR 082495) as part of a
program involving the FI pegmatite was submitted for metallurgical
testwork. Results indicate that a spodumene concentrate containing
5 - 6% Li2O at an overall recovery of 80% could be produced.
Production of a high purity lithium carbonate product was achieved
using a standard roast and acid leach process. Mica and feldspar by-
products were produced by additional flotation steps.
The Shorty (Greg) pegmatite dyke occurs in the Yellowknife Basin
within the Slave structural province. It is a member of the
Yellowknife pegmatite field, a series of pegmatites east of
Yellowknife, NWT that are probably associated with a number of late
Archean granitoid intrusions of the Prosperous Granite suite. The
pegmatites tend to occur in Burwash Formation sediments where those
have been metamorphosed to lower amphibolite facies. The pegmatites
show a broad zonation around the larger intrusives in the area; an
inner zone dominated by Be-rich pegmatites is successively enclosed
by zones dominated by Cb-Ta-rich varieties and then by Li-rich
varieties. Regional foliation in the area is parallel to sub-
parallel to bedding.  The Shorty Li-rich pegmatite intrudes medium
grade, turbiditic metasediments. It strikes 037 degrees and dips SW
at 50 - 58 degrees. The dyke is 540 m long and averages 23 m in
true thickness. A possible faulted extension can be traced for an
additional 240 m to the NE. The southern portion of the dyke
consists mainly of aplite (albite-sericite?) and narrows with depth
along with the central portion. The northern portion maintains its
thickness and grade with depth, suggesting that, to some degree,
the pegmatite plunges to the north.  The pegmatite is of the simple,
unzoned variety although banding consisting of centimetre to metre
scale alternations of medium to coarse-grained pegmatite and aplite
is common. The aplite may be an albite-sericite alteration common
in pegmatites in this area. The dyke is composed mainly of quartz,
K-feldspar, spodumene, Na-feldspar and muscovite.
Spodumene occurs as white to pale green crystals up to 8 cm long
and is preferentially developed in the coarser grained bands where
it tends to be oriented perpendicular to banding. However, near the
dyke margins, it tends to be oriented parallel to the contact.
Muscovite is concentrated near the dyke margins although it is
present throughout. Minor amounts of biotite, beryl, tourmaline and
cassiterite are present. Assays show that Ta, Be and Sn tend to
increase toward the hangingwall of the dyke.  Based on surface
sampling, trenching and 11 drill holes totalling 1261.2 m, a drill-
indicated reserve of 1.357 million tons grading 1.07% Li2O  has
been calculated. The reserve comprises a 400 m long section to a
depth of 100 m and assumes a 0.73% Li2O cutoff grade.  The Shorty
dyke was apparently called the Greg deposit (NMI) and prior to that
was Dyke A of Zone 1 on the Lit claims. Dykes B and C of Zone 1 are
parallel to Shorty. B is 240 m NW of Shorty, 330 m long, 3 m wide,
and contains medium-grained spodumene throughout. It is noted by
Fortier (1947) as a cassiterite occurrence. C is 480 m NW of Shorty,
490 m long, 9 m wide, and carries its best mineralization in the
northerly 170 m (Mulligan 1968).
The FI pegmatite dyke swarm lies within the Archean Yellowknife
Metasedimentary Basin, a vast area underlain largely by Burwash
Formation greywacke-argillite turbidites belonging to the
Yellowknife Supergroup (Henderson, 1985). These were intricately
folded and faulted during at least two phases of Archean
deformation, and metamorphosed to lower amphibolite grade in a 40
km wide, north trending zone. The Burwash sediments were invaded by
plutons, plugs and stocks of the Prosperous granite. These
discordant and predominantly north-south elongate bodies lie within
the amphibolite grade metamorphic zone and include the Hidden Lake
stock, 2 km west of the showing.  The FI pegmatite dyke swarm is a
east of Yellowknife, NWT that are probably associated with the
Prosperous Granite suite. There is a broad zonation in the
distribution of pegmatite varieties relative to the larger
intrusives in the area: an inner zone dominated by Be-rich
pegmatites is successively enclosed by zones dominated by Cb-Ta
rich varieties and then by Li rich varieties. The FI dyke swarm
lies within the Li zone.  The FI swarm contains two main
northeasterly trending and vertically dipping dykes known as the
Southwest and Main Dykes as well as a number of smaller dykes. Both
may be classified as simple pegmatites since internal zoning is not
well developed. The Southwest Dyke is discussed in a separate
report.  The Main Dyke is a branching granitic pegmatite cutting
north striking Burwash sediments. It comprises fine to coarse
grained feldspar-quartz-mucsovite with variable amounts of
spodumene. Aplitic chill zones, where present, are 15 - 45 cm thick
and spodumene poor.
The Main Dyke system can be traced for 1800 m along strike but is
most continuous along approximately 930 m. This portion is of
fairly consistent 20 m width at the north end, and splits into two
roughly equal, 425 m long branches in its southern part. The north
end is poor in spodumene (5-10%), while the southern part averages
about 15% and ranges up to 28%.  The west branch of the southern
part is 15.5 m wide and was tested by 6 trenches, concentrated near
its south end at approximately 30 m intervals. Spodumene content in
the rock exposed in these trenches ranged from 13 to 20%. Assays of
10-pound representative chip samples from the 6 trenches, including
chill zones, ranged from 0.66% Li2O across 6.1 m to 2.01% across 6.
1 m. Weighted averages across the width of the dyke ranged up to 1.
67% across 12.2 m and 1.35% across 18.3 m.  Incomplete sampling in
1975 (AR 080282) allowed a rough estimate of 7.0 million tonnes
containing 1.1% Li2O to 152 m depth in the Main Dyke. Unpublished
reports referred to in AR 082495 describe a 1978-79 program of
drilling and trenching, the results of which formed the basis for a
total FI (Main and Southwest Dykes) reserve estimate of 6,530,000
tonnes grading 1.49% Li2O to a depth of 152 m. Of this total, the
Main dyke contained 2,424,000 tonnes at 1.54% Li2O.  Five bulk
samples taken from the FI dykes in 1987 (AR 082495) were submitted
for metallurgical testwork. Results indicate that a spodumene
concentrate containing 5 - 6% Li2O at an overall recovery of 80%
could be produced. Production of a high purity lithium carbonate
product was achieved using a standard roast and acid leach process.
Mica and feldspar by-products were produced by additional flotation
steps.
The showing lies within the Archean Yellowknife Metasedimentary
Basin, a vast area underlain largely by Burwash Formation greywacke-
argillite turbidites belonging to the Yellowknife Supergroup
(Henderson, 1985). These were intricately folded and faulted during
at least two phases of Archean deformation, and metamorphosed to
lower amphibolite grade in a 40 km wide, north trending zone. The
Burwash sediments were invaded by plutons, plugs and stocks of the
Prosperous granite, and abundant related pegmatitic dykes and sills.
These discordant and predominantly north-south elongate bodies lie
within the lower amphibolite grade metamorphic zone, mostly west of
the showing. The Hidden Lake stock is exposed 7 km west of the
showing.  The showing comprises 5 Li-bearing pegmatite dykes in an
area approximately 1 x 1 km. They all strike NE and dip 45 - 70
degrees NW, cutting NE-striking, east dipping, overturned nodular
schists of the Burwash Fm. They comprise coarse grained feldspar,
spodumene, quartz and minor muscovite, and they commonly branch and
contain horses of country rock. Widths given below are surface
widths; true widths will be smaller (note the moderate dip).
Fortier (1947) notes beryl at this location also; it may be from a
small dyke just east of Dyke 12.  Dyke 12, the largest, is 300 m
long and up to 7 m wide, but is best mineralized along 200 m where
sections up to 4 m wide were estimated to contain 35% spodumene.
Banding of 25 cm pegmatitic phases with 2 cm aplitic phases is
locally well-developed. Zoning is not evident. Coarse spodumene and
feldspar crystals and streaks of grey quartz lie perpendicular to
the long axis of the dyke. It contains from 85,000 to 123,000 tons
of material, to 30 m depth, grading 1.5% Li2O.
Dyke 6 is 1100 m NE of D12, measures 170 x 9 m, and is estimated to
contain, to 30 m depth, 85,000 tons grading 1.5% Li2O.  Dyke 5 lies
1200 m NE of D12, measures 158 x 4 m, and is only locally spodumene
rich. One sample (AR 080847) contained 2.12% Li2O. Dyke 2 lies 750
m NNW of D12 and is 180 x 1.8 - 9.0 m. Dyke 1 is 900 m north of D12,
measures 100 m long by up to 11 m wide, and assayed 0.85 to 1.85%
Li2O in 6 samples. These 3 dykes carry 32,000 to 43,000 tons each,
totalling 116,000 tons to 30 m depth, grading 15% spodumene, which
is the equivalent of 1.0% Li2O (080847).
lower amphibolite grade in a 40 km wide, N-trending zone. The
Prosperous granite. These discordant and predominantly N-S elongate
bodies lie within the higher grade metamorphic zone and include the
Hidden Lake stock, 2 km west of the showing.  The FI pegmatite dyke
swarm is a member of the Yellowknife pegmatite field, a series of
pegmatites east of Yellowknife, that are probably associated with
the Prosperous Granite suite. The pegmatites show a broad zonation
in relation to the larger intrusives in the area. An inner zone
dominated by Be-rich pegmatites is successively enclosed by zones
dominated by Cb-Ta-rich varieties and then by Li-rich varieties.
The FI dyke swarm contains two main northeasterly trending and
vertically dipping dykes known as the Southwest and Main Dykes as
well as a number of smaller dykes. Both may be classified as simple
pegmatites as zoning is not well developed.  The Southwest Dyke is
a tabular, steeply dipping, 030d-striking, granitic pegmatite
cutting N-striking Burwash sediments. It comprises 15-25% pale
green spodumene as 3-6 cm crystals, 15-25% white and pink
microcline as 3-8 cm crystals and 5% muscovite. Between 40% and 60%
constitutes secondary alteration consisting of a fine-grained,
hematitic mixture of sericite and albite. This material often
occurs in alternating
The dyke can be traced for 610 m along strike and varies from 5-37
m in width. The best grades are in the central section along a
length of ~360 m averaging ~25 m in width. Spodumene content in the
central portion of the dyke averages 20% and is fairly evenly
distributed. Spodumene content decreases northward to 5%, where the
dyke contains up to 30% inclusions of country rock and is offset 3
m by a cross-cutting gabbro dyke. The southern portion of the dyke
is also less rich in spodumene and appears to be offset 9 m SE from
the central portion.  Reserves were estimated in 1975 (AR 080282)
from trench chip samples and an assumed depth of 152 m, as 4.7
million tonnes grading 1.4% Li2O. Unpublished reports referred to
in AR 082495 describe a 1978-79 program of drilling and trenching,
the results of which formed the basis for a total FI (Main &
Southwest) reserve estimate of 7,198,000 tons grading 1.49% Li2O to
a depth of 500 feet. Of this total, the Southwest dyke contained 4,
526,000 tons at 1.46% Li2O.  Five bulk sample taken from the FI
dykes in 1987 (AR 082495) were submitted for metallurgical testwork.
Results indicate that a spodumene concentrate containing 5-6% Li2O
at an overall recovery of 80% could be produced. Production of a
high purity lithium carbonate product was achieved using a standard
roast and acid leach process. Mica and feldspar by-products were
produced by additional flotation steps.
The Vo #2 pegmatite dyke occurs in the Yellowknife Basin within the
Slave structural province. It is a member of the Yellowknife
pegmatite field, a series of pegmatites east of Yellowknife, NWT
that are probably associated with a number of late Archean
granitoid intrusions of the Prosperous Granite suite. The
varieties.  The Vo #2 Li-rich dyke is a member of the Blaisdell
Lake pegmatite series. The dyke intrudes medium grade metasediments
and is more or less conformable with foliation, striking at 040
degrees with a vertical dip. It is exposed for a strike length of
about 250 m and ranges from 7 - 9 m in width. An old description
quoted in AR 080283 from GSC Economic Geology Report No. 21
describes the dyke as medium to coarse grained and banded with
respect to spodumene distribution. An analogy with other pegmatites
in the basin suggests that the banding is due to local secondary
alteration to a fine-grained mixture of albite and sericite,
commonly referred to as aplite.  Spodumene crystals are oriented
perpendicular to the dyke walls. Dark green to black crystals and
irregular masses of huhnerkobelite/triphylite are associated with
the spodumene. Scattered crystals of beryl are also present.
Apatite is reported as abundant in the Blaisdell series (DIAND
Contr. to NWT Geol., v3) but is not noted in other reports.
A reserve of 138,000 tons grading 1.62% Li2O to a depth of 100 feet
was calculated by Canadian Superior Exploration on the basis of
surface sampling and geological projection to depth.
The Vo #5 pegmatite dyke occurs in the Yellowknife Basin within the
varieties.  The Vo #5 Li-rich dyke is a member of the Blaisdell
degrees with a vertical dip. It is exposed over a strike length of
about 260 m and has an average width of about 25 m. An old
description quoted in AR 080283 from GSC Economic Geology Report No.
21 describes the dyke as indefinitely banded, with aplitic
(sericite-albite alteration) phases. Better grades of spodumene are
found in the coarser grained portions of the dyke and grade
diminishes towards the southwest end, where aplite is more abundant.
Small white beryl crystals are fairly common near the north
contact, in association with quartz and pink cleavelandite. One
greenish mass was tentatively identified as triphylite. Apatite is
reported as abundant in the Blaisdell series (DIAND Contr. to NWT
Geol., V.3) but is not noted in other reports.
A reserve of 150,000 tons grading 1.55% Li2O was calculated in 1975
by Canadian Superior Exploration based on six surface samples and
geological projection to a depth of 100 feet. The same company
drilled two short holes in 1978 showing that the dyke narrows
somewhat with depth. No new reserve was reported.
Mahe is a gold-bearing, quartz breccia hosted in a folded,
carbonaceous, sulphide-rich siltstone.  The showing is situated in
Archean aged rocks of the Yellowknife Supracrustal Belt.
Exploration work, including both surface and undergrounding
drilling,  has defined the deposit size as being 305 metres long, 6
to 30 metres wide and extending to a depth of 121 metres (GNWT RWED,
MOG Book (1997))..
This showing has been subjected to intermittant exploration from
1938 to 1987 in the form of: geochemical sampling, geological
mapping, diamond drilling and in 1974 a 350 foot deccline was
driven with one level (250 feet) and sampling. In 1984-85,
trenching, sampling and diamond drilling was done and, in 1987,
diamond drilling, geophysics and decline rehabilitation took place.
Resources calculated (1974) are listed at 64,265 tons at 0.157 oz/t
gold and some(?) silver.  In this showing gold is associated with
sulphides (arsenopyrite-pyrrhotite-galena-pyrite-chalcopyrite-and
sphalerite) in elongated quartz masses and stockwork, spatially
related to a S-shaped fold near a fault in the greywacke and slates
of the Archean Yellowknife Supergroup.
The Mitchell Lake showing has been subjected to strippong,
trenching, diamond drilling and bulk sampling. Resources calculated
(possible) are listed as 3,000 tons at 1.5 oz/t gold to 120 feet.
Gold mineralization is in shear hosted quartz veins in schists and
argillites of the Archean Yellowknife Supergroup. Visible gold is
present in a mineralized lens in the No. 1 zone. This lens, having
a width of 3 m and a length of 10 m is located within the nose of a
drag fold. Gold mineralization is associated with pyrite and
arsenopyrite.
Gold mineralization occurs within quartz veins in sediments within
the Archean Yellowknife group. This showing has been subjected to
various forms of exploration since 1937 which included geochemical
sampling, trenching, and diamond drilling. A decline was driven on
the Lambert vein and a bulk sample was taken in 1987. Three
separate veins with resources are as follows: Lambert Vein: 100ft
x5.1 ft at 0.663 oz/t gold(1966), No. 14 vein: 110ftx4.3ft at 0.416
oz/t gold (1986) and No. 18 vein: 320ftx5.4ft at 0.278 oz/t gold
(1986).
Pegmatite  dykes containing beryl cut a granite plug and associated
metasediments of the Archean Yellowknife Supergroup. Pegmatite
mineralogy consists of quartz-feldspar-beryl-tourmaline and minor
columbite-tantalite, apatite and Mn-alluaudite. This showing has
been subjected to trenching and shallow diamond drilling.
The Best Bet pegmatite dyke occurs in the Yellowknife
metasedimentary basin within the  Slave structural province. It is
a member of the Yellowknife pegmatite field, a series of pegmatites
and then by Li-rich varieties.  The Best Bet pegmatite is a Li-rich
variety belonging to the Faulkner Lake series. It is approximately
100 metres long and up to 8 metres wide. It strikes 010 degrees
with a steep westerly dip and is roughly concordant with foliation
in the enclosing schist. Some shearing has taken place along the
hangingwall contact. The pegmatite is well-zoned internally, with
the following sequence from core to border:  core: quartz -
muscovite - K-feldspar core intermediate zone: K-feldspar-quartz-
spodumene-muscovite wall zone: quartz-plagioclase-muscovite border
zone: fine-grained quartz-muscovite.
In addition to the above minerals, it also contains beryl,
columbite-tantalite, amblygonite and Li-muscovite. Much of the
plagioclase has a cleavelandite habit. Most of the plagioclase-
muscovite assemblage is metasomatic and the beryl and columbite-
tantalite tend to be associated with it. Spodumene crystals and
blocks of amblygonite in the central core reach sizes of up to 2
metres and 1 metre long respectively.  The pegmatite was mined in
the past for its tantalite-columbite content.  Estimates of
spodumene content range from 25% in the northern half of the pit to
about one-half of this in the southern half. Average Lithium Oxide
contents for the spodumene are reported to be 6.49%.  In 1975
Canadian Superior Exploration claimed that the pegmatite had a
potential resource of 42,700 tons at 2.0 % Lithium Oxide to a depth
of 500 feet.  Other higher grade, lower tonnages have been
estimated by other companies from limited drilling of the pegmatite.
The Moose #2 pegmatite dyke and smaller Moose #1 dyke occur in the
Yellowknife Sedimentary Basin within the Slave Structural Province.
They are members of the Yellowknife pegmatite field, a series of
pegmatites east of Yellowknife, NWT that are probably associated
with a number of late Archean granitoid intrusions of the
Prosperous Granite suite. The pegmatites are most abundant in
Burwash Formation sediments where the sediments have been
metamorphosed to lower amphibolite facies. There is a broad
zonation in the distribution of pegmatite varieties relative to the
larger intrusives in the area: an inner zone dominated by Be-rich
pegmatites is closest to the intrusion, and is successively
enclosed by zones dominated by Cb-Ta-rich varieties and then by Li-
rich varieties. The Moose dykes are Li-rich varieties and are
members of the Faulkner Lake series.  The two dykes are 1600 metres
apart and appear to be aligned along the same structure. The #2
dyke strikes northerly and dips steeply to the west. It is about
420 metres long and up to 60 metres wide at surface. A 221 metre
strike length was drilled to a 30 metre depth, showing the average
thickness at that level to be 7.5 - 9 metres. The #1 dyke is
slightly less than 300 metres long with a maximum thickness of 10
metres. Both are internally zoned as follows: core is quartz-
spodumene-amblygonite;  wall zone is Kspar-quartz-muscovite-
cleavelandite;  border zone is quartz-muscovite.  Other minerals
present include schorl tourmaline, beryl, cassiterite, petalite and
lithiophyllite. Li mineral rich and Cb-Ta mineral rich zones are
largely mutually exclusive.
The former are concentrated in or near the central core while the
latter are concentrated in two feldspar-rich zones near the walls
and in the fine-grained border zone. The distribution of columbite-
tantalite is also zoned, with a blocky Ta-rich variety concentrated
in the border zone and a platy Cb-rich variety elsewhere. Beryl
tends to occur as white irregular crystals and masses on the order
of 20 cm across within the wall zone bordering the core.  The
quartz core is particularly well-developed in the #2 dyke, reaching
a width of about 4 metres. Large crystals and blocks of spodumene
and amblygonite reach sizes of up to 2 metres and 1 metre
respectively. Patches and stringers of metasomatic albite and
secondary muscovite are found throughout the body.  The deposit has
been mined on two occasions, the first time involving intermittent
production in the period 1946-52 by De Staffany Tantalum-Beryllium
Mines Ltd. who produced a heavy mineral concentrate. Boreal Rare
Metals Ltd. mined the deposit in the winter of 1953-54 for both
heavy minerals and amblygonite. Beryl was stockpiled during this
period. Remaining reserves are estimated at 700,000 tonnes grading
7.44% Li and 0.25% Cb (Northern Miner, 05/06/80).
The Lens pegmatite dyke occurs in the Yellowknife metasedimentary
basin within the Slave structural province. It is a member of the
varieties.  The Lens pegmatite is a Li-rich variety belonging to
the Buckham Lake East series. It is about 90 m long and up to 20 m
wide. It parallels foliation in the enclosing metasediments (quartz-
biotite-cordierite schists) and strikes north-northwesterly with a
vertical dip. Internal zoning is not well-developed. It appears to
be the most spodumene-enriched pegmatite in the series, consisting
of 25 - 30% green spodumene crystals, up to 0.5 m long, that tend
to be perpendicular to the trend of the dyke, and up to 40%
secondary alteration products comprising a finer-grained mixture of
albite and muscovite. The remainder of the dyke is made up of
quartz and muscovite. Minor amounts of beryl and columbite-
tantalite are associated with the secondary alteration minerals.  A
paramarginal resource of 102,600 tons grading 1.97% Li2O has been
estimated from surface sampling of the Lens pegmatite (Lasmanis,
1978).
The Mut pegmatite dyke occurs in the Yellowknife metasedimentary
varieties.  The pegmatite is a member of the Li-rich Buckham Lake
East series. The dyke conforms with foliation in the country rock,
striking at 050 degrees with an apparently vertical dip. It is
about 80 m long and averages 5 m in width. Most of the pegmatite is
homogeneous and contains 25-35% spodumene in rather evenly
distributed green crystals up to 30 cm in length. These tend to be
oriented perpendicular to the contacts. Spodumene content decreases
where the dyke pinches out at near its ends. Another 40% of the
dyke is made up of white and pink microcline feldspar with crystals
up to 60 cm in length. Quartz pods situated near the centre
probably represent a segmented quartz core zone. Approximately 15-
20% of the dyke has been affected by secondary alteration involving
the development of a mixture of pink, fine-grained sericite and
albite, particularly near the contacts. No Be, Cb-Ta or Sn minerals
have been found to date.  A reserve of 25,000 tons grading on the
order of 2.2% Li2O was calculated by Canadian Superior Exploration
Ltd. on the basis of surface sampling and geological projection to
a depth of 100 feet.
The Bin pegmatite dyke occurs in the Yellowknife metasedimentary
East series. It strikes at about 060 degrees and although an exact
dip is not reported, it appears to be steep. The dyke is about 125
m long, averages 12 m wide and has been offset about 20 m into two
separate bodies. The western segment contains more than 25%
spodumene, 35% white microcline as crystals up to 45 cm across, 15%
quartz and 5% muscovite in books up to 3 cm across. About 10% of
the dyke has been affected by secondary alteration to a fine-
grained mixture of sericite and albite. Minor amounts of beryl and
columbite-tantalite are reported to be associated with the
secondary minerals. The eastern segment appears to contain somewhat
less than 25% spodumene but otherwise is similar to the western one.
A reserve of 99,000 tons grading 1.75% Li2O was estimated by
Canadian Superior Exploration Ltd. on the basis of one chip sample
and geological projection to a depth of 100 feet (AR 080278).
The Thor Lake deposits are situated in the alkaline Blatchford
Lake Plutonic Complex which intrudes Archean plutonic rocks and
Archean metasediments of the Yellowknife Supergroup at the southern
margin of the Slave Province. Geological mapping by Davidson (1972,
1978) led to the recognition of several units that make up this
multiphase, sub-circular ring complex, some 23 km in diameter and
235 square km in area. Successive units range from gabbro, with
anorthosite inclusions, through leuco-ferrodiorite, quartz syenite
and granite, to peralkaline granite and syenite (Davidson, 1982).
It is convenient to consider the Blatchford Lake Complex in two
parts: the earlier, western part including the Caribou Lake gabbro,
Whiteman Lake quartz syenite, Hearne Channel granite and Mad Lake
granite, and the later, more extensive Grace Lake granite with its
Thor Lake syenite core. Rare element minerals are enriched in the
later peralkaline unit.  Isotopic determinations indicate an early
Aphebian age (2150 Ma) for the Complex (Davidson, 1982). Bowring et
al. (1984) obtained U-Pb zircon ages of 2175 +/- 7 Ma for an older
alkaline phase (Hearne Channel Granite) and 2094 +/- 94 Ma for the
younger peralkaline phase, the Thor Lake syenite.  Mineralization
is developed in the central core of the complex which is referred
to as the Thor Lake Syenite, a 30 square km oval in the centre of
the Grace Lake Granite pluton. Six varieties of syenite including a
pegmatitic phase have been identified on the basis of textural and
compositional differences. In the vicinity of the mineral deposits,
the syenite consists of a massive medium to coarse grained
assemblage of K-feldspar with interstitial sodic amphibole,
magnetite and minor quartz.
An area of late stage veining, alteration and mineralization is
centred on Thor Lake in the western part of the Thor Lake syenite.
This area contains five zones of Nb, Ta and REE enrichment along
with high concentrations of Zr, Ga, Be, F and locally Y, Th and U.
Only the Lake and T zones are of potential economic interest.  Lake
Zone The Lake Zone is a 2 square km, triangular-shaped area of dark,
altered and brecciated rock beneath and south of Thor Lake. It is
the largest of the five mineralized zones and contains Nb, Ta, REE,
Y and Zr. Two main alteration types are present: 1) an albitite and
K-feldspar-rich syenitic pegmatite resembling a chaotic breccia
that has been intensely metasomatized; and 2) a diverse suite of
rocks rich in mafic minerals such as aegirine, biotite, Fe and Ti
oxides, albite, K-feldspar and quartz. Accessory minerals include
zircon, fluorite, allanite, ferro-columbite and members of the
bastnaesite-group. The mafic rocks are also brecciated but
alteration is more intense. A body of nepheline syenite including
minerals such as sodalite, pectolite, analcite, catapleiite,
eudialyte, andradite, willemite, mesolite and natrolite has been
identified below the Lake Zone. It is in part altered, but is not
enriched in incompatible elements and is believed to be a late
stage intrusion. Twenty-nine drill holes in the Lake Zone have
outlined a resource of 65 million tonnes grading 0.03% Ta, 0.4% Nb,
1.7% combined REE and 3.5% Zr (Trueman et al., 1988).  T Zone The T
Zone trends north-northwest away from the Lake Zone for
approximately 1 km, is up to 275 m in width and extends to a depth
of 150 m. It straddles the Grace Lake Granite-Thor Lake Syenite
contact and offsets it.
Near the Lake Zone, it is dyke-like and is known as the South T
Zone. The northern end, known as the North T Zone, is a small
circular body. Some 15 lithologies arranged in concentric to sub-
horizontal shells have been recognized in the T Zone and have been
grouped into four zones. The T Zone is of particular interest for
its Be content.  The outermost Wall zone is a pink to buff
weathering, massive unit of variable texture dominated by relict
microcline, albite and minor quartz. Columbite is a common
accessory mineral and high levels of gallium are associated with
feldspars in which it substitutes for trivalent aluminum. Moving in,
the Lower Intermediate zone includes five lithologies consisting
of various proportions of quartz, biotite, feldspar, chlorite and
magnetite. Beryllium is present in the mineral phenacite. Yttrium
and rare-earth elements are in an intimate admixture of a metamict
species believed to be thorite. Niobium is in the mineral columbite,
which occurs as massive, granular and radiating spicular
aggregates. Other minerals include purple fluorite and dolomite.
The Upper Intermediate zone is transitional between the Lower
Intermediate and central Quartz zones and is similar in gross
mineralogy to the former. It differs in that polylithionite and
phenacite are particularly abundant, making this zone the most
important host for beryllium. Polylithionite is of interest for its
lithium and rubidium content. Other Be minerals include bertrandite,
gadolinite and helvite. Y and REE are present in bastnaesite-group
minerals, thorite and Th-Y silicates.  The Quartz zone occupies the
core of the North T Zone and is present in patches within the South
T Zone. It is essentially monomineralic, consisting of white and
greyish translucent quartz.
A total of 124 drill holes in the T Zone has outlined 1.6 million
tonnes grading 0.85% BeO, including 435,000 t of 1.4% BeO, 0.26%
Y2O3, plus Nd, Sm, Gd, and Ga.  Fluorite Zone The Fluorite zone is
located at the southeastern end of the Lake Zone. It is
approximately 150 m in length, up to 15 m wide and consists of a
dense, dark-brown siliceous rock with occasional pods of fluorite.
Accessory minerals include zircon, xenotime, allanite and members
of the  bastnaesite-group.  R Zone The R zone is a series of
pegmatitic lenses and patchy zones of albitization in foliated
syenite. It is about 4 km long, up to 30 m wide and is locally
enriched in Be, Th, Nb and REE.  S Zone  The S zone is subparallel
to the R zone and lies about 200 m north of it. It is 300 m long,
averages 10 m in width and consists of syenite altered to albite
and albite-polylithionite. Patchy enrichments of Be, U, REE, Y and
particularly Nb in ferro-columbite are present.  The Thor Lake area
was first staked for uranium and REE in 1970. In 1976, Highwood
Resources discovered anomalous levels of Nb and Y as well as REE.
By 1985, a 500 m long decline had been driven into the North T Zone
to facilitate bulk sampling for metallurgical testing and related
marketing studies. A feasibility study was completed in 1989, after
which Highwood s joint venture partner Hecla Mining Co. decided to
withdraw from the project, citing difficulties in securing
commitments from potential customers. The deposits remain one of
the largest beryllium reserves in the western world.
The Hid pegmatite dyke occurs in the Yellowknife metasedimentary
varieties.  The Hid pegmatite is a Li-rich member of the Buckham
Lake West series. The dyke is approximately 200 m long, up to 6 m
wide and is discontinuous. It strikes at 070 degrees and dips
steeply to the north, crosscutting foliation in the enclosing
cordierite quartz biotite schist. The pegmatite is poorly zoned,
with microcline, quartz and muscovite as the dominant gangue
minerals. Spodumene constitutes 20-25% by volume. Irregular but
strong albitization is present.  A reserve of 50,000 tons grading 1.
56% Li2O has been calculated on the basis of two surface samples
and geological projection to a depth of 100 feet (AR 080275).
The Mac or McDonald pegmatite dyke occurs in the Yellowknife
and then by Li-rich varieties.  The Mac pegmatite is a Li-rich
member of the Buckham Lake West series. The dyke is 120 m long and
averages 10 m in width. It strikes 280 degrees, dips 60 degrees to
the south and appears to be conformable with foliation in the
enclosing cordierite quartz biotite schist. Zoning is well-
developed, particularly in the central parts of the pegmatite, with
the following sequence beginning in the core and moving outwards:
1. quartz-muscovite core  2. Kfeldspar-quartz-spodumene-amblygonite-
muscovite  3. quartz-plagioclase-spodumene-muscovite  4. quartz-
plagioclase-muscovite  5. quartz-muscovite-plagioclase border zone.
The intermediate zones are the largest by volume and the core is
discontinuous, consisting of a number of separate lenses. Muscovite-
rich zones are thicker in the hangingwall area. Alteration in the
form of a mixture of albite and sericite is common, particularly in
the central part of the dyke.
Individual spodumene crystals in the Mac dyke reach lengths of 3
metres and most are larger than about 30 cm. There is a tendency
for these to be oriented perpendicular to dyke contacts. The
spodumene is relatively fresh compared with that in many of the
other dykes in the area. In addition to the lithium minerals noted
above, Jolliffe has described minor quantities of lithiophyllite.
Notable quantities of white beryl and both fine-grained equant and
platy columbite-tantalite are associated with the albite-sericite
alteration.  A reserve of 73,000 tons grading about 2% Li2O has
been estimated on the basis of two chip samples, visual estimates
and geological projection to a depth of 100 feet (AR 080276).
Although no assays of Ta/Nb are available, Jolliffe noted several
areas within the dyke, ranging in size from three to ten square
feet, in which he estimated between 1 and 2 percent tantalite.
The Norma gold prospect is situated in the Yellowknife Basin, a
supracrustal belt within the Archean Slave structural province.
Gold occurs in quartz veins hosted by turbiditic metasediments
belonging to the Burwash Formation which is part of the Archean
Yellowknife Supergroup. The sediments include medium-bedded
greywackes rhythmically interbedded with argillite and occasional
layers of grey to black, thin-bedded phyllite. The strata are
strongly deformed into folds with axes plunging steeply to the
northeast. Regional metamorphic grade is lower greenschist.
The Norma vein has been traced on surface for about
550 m. It averages 15 cm in thickness and is concordant with
bedding, following an argillite layer in the turbidites. Several
minor quartz veins parallel it nearby. It is composed mainly of
rusty weathering, grey quartz containing a variable amount of wall
rock inclusions along with minor carbonate, feldspar, biotite and
chlorite. Metallic minerals constitute less than 1% of the vein by
volume and include arsenopyrite, galena, chalcopyrite, marcasite,
scheelite and native gold. Sphalerite and pyrrhotite have been
tentatively identified. Native gold tends to occur with galena and
the other sulphide minerals, particularly near the slate wall rock,
near inclusions of wall rock, and in chloritic slips.
The bulk of better grade material is present in two main
shoots named the
Much of the hangingwall argillite in its vicinity has been strongly
chloritized, while silicification of the footwall greywacke appears
to have taken place. Also in the footwall is a 20 m wide area in
which the sedimentary strata have been strongly contorted, broken
and infilled with numerous stringers and irregular bodies of quartz.
Shoot B was reported to be about 10 m long, 0.3 m thick and to
contain in excess of 1 oz/ton Au. Shallow diamond drilling revealed
only erratic values of gold.  Discovered in 1939, the prospect has
received much exploration attention since then. High surface assays
and heavily promoted results of a drill program led to a premature
and abortive attempt at production in 1946 with a reserve estimate
of 105,000 tons grading 1.0 oz/ton Au. A total of 252 tons were
eventually milled with a production of 7.5 oz gold. In 1947, an
independent consultant (A.D. Hellens) was called in and calculated
a new reserve of 1,200 tons grading 0.65 oz/ton Au to a depth of
225 feet.
The Thor (Echo Lake, Tanco) pegmatite dyke swarm occurs in the
Yellowknife Basin within the Slave structural province. It is a
and then by Li-rich varieties.  The Thor swarm is a Li-rich member
of the Thor-Echo series. Numerous northwest striking and steeply to
vertically dipping pegmatite dykes occur in an area about 1200 m
long and 650 m wide. Both zoned and unzoned types are present
although the latter are most common. They have been divided into
four groups as follows:  WEST  Approximately 45 m long and up to 5
m thick, this dyke is well-zoned, grading from a quartz - spodumene
? K-feldspar core through a plagioclase - K-feldspar - muscovite -
quartz ? spodumene intermediate zone to a plagioclase - muscovite -
quartz wall zone. Spodumene crystals are generally oriented
perpendicular to the contacts. Alteration to a fine-grained mixture
of albite and sericite is widespread. Beryl, columbite-tantalite,
apatite and altered triphylite are associated with alteration.
TANCO  This dyke lies along strike from the WEST dyke and is about
180 m long and up to 8 m wide. It is relatively homogeneous,
consisting mainly of quartz, albite and minor muscovite.
Blocky K-feldspar, spodumene and amblygonite are dispersed
throughout the dyke but are more abundant in the central portions.
Beryl and columbite-tantalite are generally found with them.
CENTRAL  This swarm consists of two sets of dykes with slightly
differing orientations. A northwest trending set is generally
unzoned, with spodumene and K-feldspar oriented perpendicular to
dyke margins. Alteration to fine grained albite-sericite is present
although beryl, columbite-tantalite and phosphate minerals are rare.
A northeast trending set of dykes connects or bridges the
northwest set and is characterized by unoriented K-feldspar and
spodumene as well as a lack of alteration and the absence of rare
element mineralization.  EASTERN  The eastern set strikes
northwesterly and dips steeply to the northeast. Internal structure
varies from completely unzoned to well-zoned along the length of
the dykes. Spodumene content varies from abundant to absent and Nb-
Ta and Be mineralization is rare.  Various phases of exploration
have been carried out since the mid-1950 s, including trenching,
bulk sampling and some diamond drilling. A reserve of 1.84 million
tons grading 1.5% Li2O based on surface sampling and geological
projection to a depth of 100 feet has been calculated by Canadian
Superior Exploration (AR 080478).
The Big Hill East pegmatite dyke swarm, also known as the BA or
Murph, occurs in the Yellowknife metasedimentary basin within the
varieties.  The Big Hill East pegmatites are Li-rich varieties
occuring in a northeasterly trending dyke swarm that cuts the trend
of bedding in the host metasediments at a low angle. The swarm has
a strike length of 1070 m and a width of about 150 m. Individual
dykes are up to 15 metres wide. Immediately north of this swarm,
the Big North swarm probably represents a faulted off extension of
the Big Hill East.  The pegmatites are classified as simple rather
than zoned, since crystals are generally a few centimetres across
and the various minerals are distributed relatively evenly
throughout. In order of abundance, the minerals present are:
microcline, spodumene, quartz and muscovite. In the larger dykes,
spodumene generally occurs as pale green crystals averaging 8 cm in
size which tend to be oriented perpendicular to the contacts and
dip east at 10 - 30 degrees. However, both microcline and spodumene
occur as crystals up to 0.5 m across locally. A secondary, fine
grained plagioclase-muscovite alteration is common, constituting as
much as 30% of the dykes in places.
Where present, it has also affected spodumene and greatly reduced
its abundance. The alteration is particularly common where dykes
finger out and may be somewhat more abundant in the Big North swarm.
Reserves are estimated (AR 080273) at 3.1 million tons grading 1.
5% Li2O to a depth of 150 m. One old drill hole from the 1950s (AR
082348) showed the dykes to remain constant in width to that depth.
At the Big North swarm, the same report estimates a reserve of 160,
000 tons grading 1.27% Li2O to a depth of 30 m.
The Jake pegmatite dyke swarm occurs in the Yellowknife
and then by Li-rich varieties.  The Jake dyke swarm consists of 15
generally northwesterly striking pegmatite dykes of the Li-rich
variety, each up to 5 m wide and 1000 m long and all contained
within an area about 1 km by 1.2 km. Unlike many of the other
members of the Yellowknife pegmatite field, these are hosted by
intrusive granodiorite of the Defeat Plutonic Suite rather than
metasediments. The dykes are immediately northeast of the Paint
dyke swarm and may in fact be related to them.  Although some of
the dykes exhibit a quartz core, in general they are not well-zoned
and can be classified as simple. Mineralogy is similar throughout
the swarm although the proportions of minerals in each vary to some
degree. The Jake #1 dyke is described in most detail and consists
mainly of white, euhedral feldspar, quartz and muscovite together
with about 10% spodumene and minor amblygonite. Spodumene occurs as
colourless to pale green-grey, zoned crystals up to 30 cm long that
are generally oriented perpendicular to the contacts with host
granodiorite.
Spodumene tends not to occur in the margins of the dyke.
Amblygonite is greyish-white and typically contains small amounts
of pale blue lazulite. Feldspar crystals occasionally contain minor
amounts of platy tantalite-columbite. Other minor accessory
minerals include yellow-green apatite, galena, cassiterite and
possible wolframite.  Five of the thirteen dykes contain
significant amounts of spodumene. A 1981 assessment report (AR
081352) calculates a reserve of approximately 2.1 million tonnes
grading 1.12% Li2O on the basis of surface sampling, visual
estimation and geological projection to a depth equivalent to 1/2
of the sampled strike-length (maximum of 380 m). Two more dykes
were described as potentially interesting but having lower visual
estimates of grade.
The Paint pegmatite dyke swarm occurs in the Yellowknife
and then by Li-rich varieties.  The Paint Li-rich dyke swarm
consists of four northwesterly striking and steeply southwesterly
dipping pegmatite dykes up to 1.6 m wide and 1000 m long. Unlike
many of the other members in the Yellowknife pegmatite field, they
are hosted by intrusive granodiorite of the Defeat Plutonic Suite
rather than metasediments. They are immediately southwest of the
Jake swarm and may in fact be related to them.  The spodumene-
bearing dykes are not zoned and may be classified as simple,
although a number of smaller, non-lithium rich dykes in the
vicinity are well-zoned. The gangue mineralogy of the dykes is not
discussed in available references other than mentioning the
presence of pink feldspar. Spodumene and much lesser amblygonite
are the only potentially economic minerals.  Accessory minerals
include columbite-tantalite, sphalerite, galena and cassiterite.
Spodumene occurs as large, light green crystals usually oriented at
high angles to dyke contacts. On surface, these have been altered
to a chalky white colour.
Amblygonite occurs in amounts of up to 5% as small patches lacking
crystal form. It is also found in one of the smaller, zoned and
presumably unrelated pegmatites.  A reserve of 2.774 million tonnes
grading 1.75% Li2O was calculated in AR 081137 on the basis of
crystal counting (with some check assays) and geological projection
to a depth of 500 m. A 100 kg bulk sample was submitted to
Lakefield Research for metallurgical testing. The results showed
that a high grade lithium concentrate assaying 6.2% Li2O could be
produced at a recovery of 87%.
The Ann (Reid Lake) pegmatite dyke occurs in the Yellowknife
and then by Li-rich varieties.  The Ann dyke is a Li-rich variety.
It strikes at 130 degrees, dips steeply to the south and is roughly
conformable with foliation in the enclosing metasediments. It has
been traced on land and under a lake by drilling for a strike
length of 1200 m and has an average thickness of 12 m. The
pegmatite is unzoned, consisting of grey plagioclase, milky to grey
quartz, a variable amount of pink feldspar and scattered books of
muscovite. Spodumene occurs as platy greenish grey crystals up to
25 cm long. Amblygonite is reported and the presence of high Li2O
assays in the absence of spodumene suggests that it may be
relatively abundant.  Drilling in 1956 (AR 082243) intersected the
dyke at depths of over 100 m and demonstrated continuity in width
and grade. A possible reserve of 3,335,600 tons grading 1.92% Li2O
is reported in Canadian Deposits Not Currently Being Mined (1989);
estimate is from Lasmanis (1978).
The Cassidy Point deposit lies near the western edge of the Archean
Yellowknife Metasedimentary Basin, a vast area underlain largely by
Burwash Formation greywacke-argillite turbidites belonging to the
Yellowknife Supergroup (Henderson, 1985). These were folded and
faulted during at least two phases of Archean deformation, and
metamorphosed to lower amphibolite grade in a 40 km wide band
including the Cassidy Point deposit. The deposit lies approximately
3 km west of a north-south elongate pluton belonging to the Archean
Prosperous granite, which is a group of plutons and smaller bodies
of massive, unmetamorphosed granite, and abundant related pegmatite
dykes.  The deposit is an auriferous quartz vein system within a
shear, cutting folded metagreywackes and incipiently nodular
schists of the Burwash Formation. The sediments in the southern
Prosperous Lake area have been folded about moderately to gently SE-
plunging and moderately to steeply NW-plunging axes, while the
auriferous zone trends NE/40 degrees NW (MIR 81). According to AR
081344, the veins occupy a shear folded into a syncline plunging
gently along an east-west axis; this plunge, and the dips of the
shear
Numerous grab samples from the main pit have assayed over 30 g/t Au.
Typically, gold values increase with sphalerite content, and a 0.5
m drill intersection in 1955 assayed 26 g/t Au and 4.4% Zn. A 0.2 m
intersection assayed 32 g/t Au and 26.2% Zn, and a 1.2 m section
assayed 0.12% Zn, 2.4% Pb and 20 g/t Au.  A bulk sample weighing
1112 tonnes was taken from a decline driven into the main vein in
1986, and was processed at the Con mill, where a 97.12% recovery
was attained. The ore averaged 12.7 g/t Au. The latest reserve
estimates are from 1981 (AR 081344) and state proven reserves of
1400 tonnes grading 15.43 g/t Au, amenable to open pit mining with
a strip ratio of 4:3.
The Vega showing or deposit lies near the western side of the
Archean Yellowknife Metasedimentary Basin, a vast area underlain
largely by Burwash Formation greywacke- argillite turbidites
belonging to the Yellowknife Supergroup (Henderson, 1985). These
were folded and faulted during at least two phases of Archean
deformation (Fyson 1987, Brophy 1987), and metamorphosed to lower
amphibolite grade in a 40km-wide band including the showing. The
showing lies ~2.5km SW of a N-S elongate pluton belonging to the
dykes, which invaded the Burwash sediments in the late Archean.
Jolliffe (1941) shows a Au occurrence in a NW-trending vein on the
south side of McKeekan Bay, the southern bay of Prosperous Lake
(GSC Map 868A). Assessment records show that trenching and drilling
tested two quartz veins here in 1944, one of the south side of
Mckeekan Bay striking NW for 128m, and one on the north side, 300m
NNE of the first, striking WNW for 106m. The northern one was
opened in 5 trenches. Another trench tested a target inbetween the
two veins (another vein?). The southern quartz vein coincides with
Jolliffe s gold occurrence and was tested with 6 trenches. Five
holes were drilled along 400m including the south vein and the area
to its north. A sixth drill hole was collared on a small island in
the Bay roughly 750m SE of the vein exposure.  Results of this work
are not available, but in a report dealing with the Tom and
Ptarmigan Mines property, 1500m SW of Vega, the Vega is referred to
as a deposit for which small reserves of gold ore were outlined,
presumably in the late 1940s.
Nearby deposits such as Tom, Ptarmigan and Cassidy Point are hosted
by discordant quartz veins mineralized with pyrite, sphalerite,
galena and locally other sulphides, cutting turbiditic
metasediments near NNW-trending, Early Proterozoic sinistral faults.
The showing occurs in the Yellowknife (YK) Volcanic Belt. This
Archean supracrustal belt trends north for roughly 8.5 km and
includes a 10 - 12 km thick, tholeitic basal sequence, the Kam
Group, overlain by 2 km of dominantly calc-alkaline volcanics and
turbiditic sediments of the Banting Group. The volcanic belt is a
SE-facing, steeply dipping homoclinal sequence, flanked on the east
by a vast basin of Archean turbiditic metasediments, intruded to
the west by the Archean Western Plutonic Complex, and cut by
Proterozoic diabase dykes of the Dogrib and Indin generations.
Regional metamorphism in the belt does not exceed greenschist
facies, except adjacent to the Western granodiorite. The entire
belt has been subjected to compressional stress that is manifested
by anastomosing, high-angle, reverse shear zones (Lewis 1987, MDD
GAC YK Field Guide p191). These early shears are pre-diabase in age,
and host most of the gold mineralization discovered to date in the
belt. A set of regional, Proterozoic sinistral faults post-date the
diabase; one of these is the Akaitcho Fault, which strikes NW just
south of the deposit.  The four formations of the Kam Group
comprise predominantly mafic volcanics with minor amounts of
dacitic volcanics and tuffaceous sediments, intruded by metagabbro
sills and sheeted dykes. The Crestaurum Formation, second from the
base, is regionally characterized by massive and pillowed basalts
or andesites with a number of laterally continuous felsic horizons,
invaded by synvolcanic(?) metagabbro sills and cut by a N-trending
swarm of metagabbro dykes (Padgham 1987; MDD GAC YK Field Guide
p11). The overlying Townsite Formation, on the other hand,
comprises dacitic pyroclastics intruded by metagabbro dykes and
sills, particularly one large sill which invaded the central part
of the Formation.
On the property, the stratigraphy strikes 030 - 050 degrees and
dips 70 - 85 degrees east except in the vicinity of the west zone
where dips are 75 - 85 degrees west.  At the showing, massive,
pillowed and variolitic andesites of the Crestaurum have been noted
in the hangingwall of the west zone. Porphyritic dacite and the
major, central gabbro sill of the Townsite Formation form the
footwall, and a younger? (AR 082156) gabbro of the Townsite
Formation hosts the east zone. The volcanics have been
metamorphosed to lower greenschist facies, consisting of chlorite
and epidote after hornblende, hornblende after pyroxene, and
epidotized feldspar.  The anastomosing shear system which hosts the
ore at Giant Mine, to the south, is apparently displaced 1900 m NW
by the Akaitcho Fault, to continue as the Lynx west zone. The Lynx
shear system has been described as a west-dipping west zone, and a
subsidiary, gently east-dipping east zone, forming an anticlinal
geometry similar to that seen at Giant Mine, but with the crest of
the anticline removed by erosion. The Lynx deposits occur north of
Gold Lake and south of Vee Lake, but the NT MINFILE showing
Supercrest GKP Zone, just south of Gold Lake, partially underlies
the Lynx property and is geologically part of the Lynx system.  The
east zone shear strikes NE and dips 20 degrees SE. About 100 m
north of Gold Lake, where the shear is approximately 100 m wide, a
SW-plunging synclinal undulation in it hosts the Original Discovery.
The Discovery comprises two strongly sheared, carbonatized and
silicified auriferous zones along the boundaries of the shear.
South of the Original Discovery, the Lynx Fault, a west-trending
dextral splay of the Akaitcho Fault, probably displaces the zone
275 m west, from which point it continues south to the Akaitcho
Fault (AR 082156).
Its total length is roughly 730 m, and it has been traced down-dip
an unknown distance. About a kilometre NE of the Discovery, minor
gold values are present in chlorite-sericite schists in the NE
extension of the east zone (NMI Au 09). Grades and sizes in the
east zone were sub-economic in 1965 (AR 082156).  The west zone
occurs along the locus of the Vee Lake fault, an early (pre-
diabase) thrust fault with unknown vertical displacement and 1500 -
3000 m horizontal displacement. It strikes 010 - 020 degrees and
dips 70 - 75 degrees west, partially along the west side of the
Townsite central gabbro sill and partially along the Townsite -
Crestaurum contact. The fault extends 7 km, from the Akaitcho Fault
south of Gold Lake, through Vee Lake to the Hay-Duck Fault at
Jackson Lake, and is variably sheared along its length. It crosses
through Townsite dacites and metagabbros in the showing area, and
Crestaurum andesties and metagabbros north of Vee Lake. Drilling
has tested the west zone shear along most of the 1km between Gold
and Vee Lakes to an unknown depth. It comprises chlorite +/-
sericite schist. Mineralized lenses within this part of the shear
are small, and comprise lenses and veins of quartz +/- carbonate,
mineralized with pyrite +/-arsenopyrite and gold. The gold occurs
with the sulphides or as free gold. Good grades have been
encountered over narrow widths (Knutsen 1974). The zone has also
been drill-tested beneath Vee Lake (by different operators, working
the PRW claims) with negative results (NMI Au 10 and AR 061044).
In 1977 the west zone was judged to have a small open pit potential
(NMI Au 08).
The Big Hill West dyke swarm, also known as the BA or Murph, occurs
in the Yellowknife metasedimentary basin within the Slave
structural province. It is a member of the Yellowknife pegmatite
field, a series of pegmatites east of Yellowknife, NWT that are
probably associated with a number of late Archean granitoid
intrusions of the Prosperous Granite suite.  The pegmatites tend to
occur in Burwash Formation sediments where those have been
metamorphosed to lower amphibolite facies. The pegmatites show a
broad zonation around the larger intrusives in the area; an inner
zone dominated by Be-rich pegmatites is successively enclosed by
zones dominated by Cb-Ta-rich varieties and then by Li-rich
varieties.  The Big Hill West pegmatites are Li-rich varieties that
occur in a northeasterly trending dyke swarm, cutting the trend of
bedding in the host metasediments at a low angle. The swarm has a
strike length of 1280 metres and a width of about 150 metres. It
consists of four main subparallel dykes which are each up to 20
metres wide. The pegmatites are classified as simple rather than
zoned, since crystals are generally a few centimetres across and
the various minerals are distributed relatively evenly throughout.
Minerals present, listed in order of abundance, are: microcline,
spodumene, quartz and muscovite. A secondary, fine grained
plagioclase-muscovite alteration is common, constituting as much as
50% of the dykes in places. It has affected spodumene and greatly
reduced its abundance in places. The alteration is particularly
common where dykes finger out. Although most of the dykes contain
abundant spodumene (up to 30% by volume), some contain less than 5%.
Reserves are estimated (AR 080273) at 1.3 million tons grading 2%
Li2O although the writer felt that the number of samples taken was
too low to justify this grade figure. He noted, however, that
drilling in the 1950s (AR 082348) proved that the dykes continued
to at least a depth of 150 metres. In 1979, Canadian Superior
returned to excavate 13 new trenches. No new reserve figure was
estimated (AR 080957). Lasmanis (1978) estimates 7,888,000 tons of
rock grading 1.47% Li2O under the property, which includes the Big
North and Big Hill East deposits.
The showing occurs in the Western Plutonic Complex where the
plutonic rocks invade the western edge of the Yellowknife Volcanic
Belt. This belt is a north trending, steeply dipping sequence of
Archean Yellowknife Supergroup volcanics and minor sediments. The
Complex along its western margin comprises felsic intrusions of at
least five ages, each mappable in a distinct terrane, forming a
body of batholithic proportions ranging from gabbro-tonalite to
trondhjemite-granodiorite-granite in composition. The Belt and the
Complex are cut by Proterozoic diabase dykes of two or three
generations. Regional metamorphism in the Belt achieved lower
amphibolite grade adjacent to the Plutonic Complex. Regional, high-
angle, reverse shear zones within the Belt locally host significant
gold deposits (eg. Giant Mine, Con Mine) but do not cut the Complex.
Later Proterozoic faults cut both the Belt and the Plutonic
Complex, locally displacing their mutual contact on a regional
scale.  The showing is 4.5 to 5.0 km west of Yellowknife Bay and
just SW of Baker Lake, in an area underlain by massive, fine to
coarse-grained, grey and pink biotite granodiorite intruded by
pegmatite and aplite and locally containing volcanic inclusions.
Areas of the host granite containing volcanic inclusions appear to
be important to mineralization (GSC P 65-11). According to Atkinson
and van Breeman s (DIANDEO 90) descriptions, the host unit must be
part of the Upper Defeat Suite phase, a series of homogeneous,
porphyritic, biotite trondhemite-granodiorite-granite lobes
representing the late uppermost level of the Defeat Suite, and
invading the Volcanic Belt at the eastern edge of the Complex. The
Martin Fault, a regional Proterozoic fault, cuts NW through Baker
Lake about 1 km NE of No.15 and 1.4 km NE of No.22.
Gold is hosted by various altered, quartz-filled fractures,
fracture zones, and shear zones, the main ones being Veins No.15,
No.22 and No.11S. The zones are generally consistent in width but
do vary, from one narrow crack to a 3.5 m wide shear. The wallrock
is invariably hematized, for 0.3 to 1.0 m from the zone. The main
zones in the area comprise sheared quartz in pinched out lenses,
stringers and pods, often ribboned with aplitic material, and
surrounded by sheared granitic and aplitic rocks (GSC P 64-22).
The quartz is lightly mineralized with pyrite and hematite (less
than 1% combined), and locally galena, chalcopyrite and sphalerite.
Gold occurs free and associated with sulphides, and visible gold
has been observed in numerous different zones on the Rodstrom
property (see also J Group and C Group).  No.15 Vein is the object
located by the given coordinates. It has been exposed along 55 m at
NE/65E, with possible extensions 50 m NE and 45 m south. The
innumerable quartz lenses comprising the Vein yielded encouraging
gold values in trenches along a 24 m length in 1963 (GSC P 64-22),
and drilling of 2342 m in 57 holes in 1964 defined a 33.5 m long
shoot at about 7.5 m depth, which averaged 46.6 gpt Au across 1.1 m.
Interest in the showing waned until it was re-staked in 1975.
Reserves for No.15 were calculated in 1976 at 843 tonnes grading 49
gpt Au across 1.1 m, with additional inferred reserves of 1397
tonnes grading 28 gpt Au across 1.1 m (MIR 1976).  The No.22 Vein
is about 550 m WNW of No.15. It is exposed along 37 m at 050/45 -
50dSE, and is traceable for several hundred fee, possibly more than
a thousand feet (300 m).
Surface sampling after its discovery in 1964 indicated an average
grade of 93.9 gpt Au across 0.8 m for a length of the vein (GSC P
65-11); re-evaluation in 1975/76 resulted in calculated reserves of
141 tonnes at the same grade and width (MIR 1976). The No.22 Vein
contains a greater proportion of chloritic volcanic inclusions at
depth (GSC P 65-11).  The No.11S Vein lies between the other two,
about 450 m NW of No.15. Parts of it are said to contain lenses of
high-grade material (GSC P 65-11).  A 1976 test by Cominco Limited
on a sample of ore grading 77.6 gpt Au (presumably from No.15)
showed a 99.07% recovery using standard cyanidation techniques.
The Cab (Gar) Bi-Co-Cu-Au deposits are located in the southern
Great Bear Magmatic zone, a 1.88-1.86 Ga zone of calc-alkaline,
mainly intermediate, subaerial volcanic and plutonic rocks within
the Wopmay orogen. Mineralization occurs in a northwesterly
trending belt of Aphebian Snare Group sediments which are
unconformably overlain by rhyolitic volcanic rocks related to the
Great Bear Zone. The rhyolites and related volcaniclastic rocks are
relatively undeformed and are tilted gently to moderately to the
north. All stratified rocks are surrounded by granodiorite, quartz
monzonite and granite intrusives of the Great Bear Zone. Snare
Group rocks are metamorphosed to greenschist facies.  Bi-Co-Cu-Au
mineralization is hosted within metasediments of the Snare Group
which strike northwest and dip steeply to the northeast.
Lithologies are broadly divided into a relatively uniform, fine
grained, thinly bedded siltstone and a more variable unit of
quartzite-argillite. The latter includes massive quartzite which
grades into thinly bedded argillites containing variable amounts of
chlorite and/or magnetite as laminae. These have been interpreted
by some as oxide facies iron formations and in places grade from a
magnetite-rich base up into a chlorite-biotite rock and then into
argillaceous quartzite. In the deposit area, one of these horizons
has been traced over a 1 km strike length and varies in thickness
from a few centimetres to 2 m. A second chlorite-rich unit higher
in the section includes thinly bedded dolomite. Chlorite-rich
horizons are often complexly and tightly folded.
All major sulphide occurrences are associated with the chlorite-
rich rocks. Arsenopyrite is the predominant sulphide and occurs as
disseminations, coarse-grained aggregates of subhedral to euhedral
crystals, and veins. In chlorite-rich horizons, it forms thin
layers and lenses parallel to bedding while in more competent
quartzite it tends to occur in cross-cutting veins or fracture
zones. Where chlorite-rich rocks are strongly folded, it may occur
as cross-cutting veinlets. Disseminations occur in both rock types.
Pyrite and chalcopyrite occur as coarse aggregates with
arsenopyrite in places. Bismuth minerals, including mainly
bismuthinite, native Bi and emplectite, are present in small grains,
either interstitially in arsenopyrite aggregates or within
arsenopyrite crystals. Cobalt is present mainly within the
arsenopyrite lattice and to a much lesser extent as small grains of
cobaltite.  Many of the occurrences are cut by feldspar porphyry
dykes and arsenopyrite appears to have been remobilized into
fractures within the dykes as well as into massive podiform
accumulations within layered rocks near the dyke margins. The
maximum strike length of any of the showings is on the order of 100
m and some reach a maximum width of about 10 m. Many consist of
several sub-parallel zones.  New Athona Mines Ltd. outlined two
main zones of mineralization with trenching and drilling in the
late 1960 s. Based on this work, they reported a reserve of 194,700
tonnes grading 0.162% Bi and unspecified levels of Cu, Co and Au in
the No. 1 zone.  The No. 2 zone is a 3 m wide zone of massive
arsenopyrite with very short strike length from which individual
samples returned values of up to 0.21 opt Au, 0.66% Bi and 3.28% Co.
Sue (commonly known as Sue-Dianne) is an Olympic Dam-type
mineralization containing copper, uranium, gold, silver and iron
concentrations.  Ore minerals occuring on the showing include
chalcopyrite, bornite, chalcocite and pitchblende.  The deposit
occurs in a pipe-like, magnetite cemented, brecciated horizon
comformable with a package of thick ash flows.  These rocks are
situated on the eastern side of the Bear Structural Province
(Proterzoic aged rocks) within the Great Bear Magmatic Zone.  The
property operated through a joint venture between Fortune Minerals
NWT and Noranda Inc. (GNWT RWED, MOG Book (1997)).
The Lou Lake showing is a gold, bismuth, cobalt, copper and
tungsten oxide showing  occurring within 4 kilometres south-
southeast of Lou Lake.  The showing, comprise of three closely
spaced mineralized zones (Summit Peak, Bowl and Nico Lake),  occur
in 1 to 65 metre stacked lens of black rock schists and breccias
with variable mineralization.  These lens are stratabound and
strike southeast for approximately 900 metres (GNWT RWED, MOG Book
(1997)).
The Camp Lake gold showing consists of auriferous lenticular zones
containing sulphide bearing (pyrite, pyrrhotite, arsenopyrite,
sphalerite, galena and chalcopyrite) in stringers within shear
zones which are conformable with greywackes of the Archean
Yellowknife Supergroup. Diamond drill indicated resources of 51,150
tons at 0.40 oz/t OR 13,050 tons at 0.35 oz/t gold are listed.
1938 to 1981. Work included: surface exploration, sampling, diamond
drilling and a feasibility study (1981).
The Slemon showing is underlain by Archean Yellowknife Supergroup
sediments and intrusive quartz porphyry sills which contain gold
bearing quartz veins, stockworks and breccia zones. The latter
contain gold bearing bands of massive pyrite plus some silver and
bismuth tellerides. Possible mineral resources are listed at 35.000
tons at 0.2 oz/t gold OR 60,000 tons at 0.4 oz/t gold using diamond
drill sludge samples.  This showing has been subjected to sporatic
exploration from 1939 to 1987. Work included trenching, diamond
drilling, test pitting, soil sampling, mapping, pitting and bulk
sampling.
Regional The region is predominantly underlain by massive
greywackes and minor argillites of the Archean Yellowknife
Supergroup which strike NNE and dip nearly vertically. A band of
mafic to intermediate volcanics several hundred meters wide,
extends along the east side of Goodwin Lake, while chloritic tuffs,
mixed with greywackes occur near Barker Lake. Coarse grits to
pebble conglomerate were observed locally. Bedding tops generally
point to the west.  Conformable with the stratigraphy are a number
of medium grained quartz diorite sills. Contacts are often not too
sharp because of the fine grained chill margin and alteration of
the enclosing sediments. Many showings are located in proximal to
these sills. An erratic distribution of diabase dykes occur on the
property as a late stage post mineralization event.  Two stages of
deformation have affected the stratigraphic sequence, resulting in
tight isoclinal folds with very steep plunges and long limbs that
are nearly vertical. Usually only minor flexures such as small drag
folds and minor strike slip faults are observed near the fold noses.
Metamorphism is of the lower greenschist facies.
Property The claims are underlain by sedimentary rocks which are a
series of interbedded, fine-to-medium grained greywackes and
argillites of the Yellowknife Supergroup which strike NNE and dip
nearly vertical. A band of mafic to intermediate volcanics several
hundred meters wide extends along the east side of Goodwin Lake,
while chloritic tuffs mixed with greywackes occur near Barker Lake.
Coarse grits to pebble conglomerate were observed locally. Bedding
tops generally point to the west.  Conformable with the
stratigraphy are a number of medium grained quartz diorite sills.
Contacts are often not too sharp because of the fine grained chill
margin and alteration of the enclosing sediments. Many of the
showings are located in proximity to these sills. An erratic
distribution of diabase dykes occur on the property as a late stage
post mineralization event.  The host of the deposit is a quartz
diorite sill which intrudes these sedimentary rocks. The sill
outcrops at intervals for a length of 2,400 feet and varies from 15
to 60 feet in width. It strikes nearly north 35 degrees east and
dips about 80 degrees southeast parallel with the enclosing strata.
Showing The diorite host sill contains rounded fibrous clots of
amphibole from one sixteenth to one eighth of an inch in diameter.
Minute grains and blebs of pyrrhotite occur throughout, and
together with a little pyrite, comprise several percent of the rock.
Quartz bodies cut the diorite and generally do not extend into
the adjacent strata. The quartz is commonly concentrated near or at
the walls of the sill, particularly the northeast wall. The quartz
is light and dark grey and mottled, and adheres firmly to the wall
rock. It occurs as veins and irregular masses ranging from an inch
to several feet in width.  Metallic minerals, comprising less than
one percent of the vein matter, are mainly arsenopyrite, pyrite,
and pyrrhotite: others noted are galena, chalcopyrite, and
sphalerite. Gold is reported in the quartz and in the adjacent
diorite. Both the quartz bodies and enclosing quartz diorite are
cut by rare veinlets of drusy white calcite and possibly pyrite.
Exploration The main zone was trenched and was tested by 13,600
feet of diamond drilling. In 1947 a shaft was sunk to a depth of
160 feet. It is inclined at 65 degrees in the direction N 35
degrees E. Underground development was done on the 150 foot level
and the mined material was sent to Yellowknife for assay. Some
diamond drilling was done underground. No results from trenching or
diamond drilling could be located. The economic potential for this
showing was calculated at 700 tons per vertical foot at a gold
grade of 0.60 oz/ton.
Regional  This Showing is in the Russell Lake - Slemon Lake
Supracrustal belt. These rocks are part of the Archean Slave
Province. Supracrustal rocks include minor amounts of mafic and
felsic metavolcanics and abundant greywacke-mudstone metasediments,
which represent a turbidite sequence similar to that found
elsewhere in the Slave Province. The metasedimentary succession at
Russell and Slemon lakes is characterized by abundant oxide and
silicate amphibolitic iron formation that is locally sulphide rich
(pyrite, pyrrhotite and arsenopyrite) and auriferous.  The
supracrustal rocks have undergone at least three phases of folding,
with F1 and F2 isoclines refolded about more open F3 folds. Three
foliation subsets post-date F2 isoclines. Two major sets of post-
Archean faults transect the area: N-NW trending sinistral faults
and easterly trending dextral faults. Quartz and quartz-carbonate
veins were injected througout the deformational history of the area.
Metamorphic grade ranges from greenschist to amphibolite facies.
Within the metasedimentary rocks this transition is marked by a
regional cordierite isograd. The isograd parallels the contact
between the supracrustal rocks and the bounding granitic rocks and
is offset by post-Archean faults. (MIR 1986-
87)
Property/Showing  A thick mafic intrusion cuts metasediments north
of the Bugow deposits. All stratified rocks have been metamorphosed
to at least upper greenschist facies and in the area of the
deposits, to lower amphibolite facies. Structure in the area of the
deposits is complex, recording at least two periods of folding.
The Bugow iron formation is the most significant of several iron
formations situated within a sequence of turbiditic metasediments.
In general, sediments underlying it are more psammitic and those
above it, in which the minor iron formations are situated, are more
pelitic. Intercalated with and enclosing the iron formations are
black pelitic schists containing garnet, chlorite and quartz. A
locally tuffaceous, intermediate to mafic volcanic unit underlies
the metasediments. Numerous small pegmatites intrude both iron
formation and metasediments and a large mafic intrusive has been
intersected in drill core.  The iron formations are well-laminated
and have been divided into a silicate facies and silicate-sulphide
facies on the basis of sulphide content. Both are characterized by
alternating laminae of chert and various proportions of grunerite/
hornblende, garnet, chlorite, and sulphides together with minor
iron oxide and carbonate. Silicate-sulphide iron formation is also
distinguished by a larger proportion of cross-cutting quartz veins,
an increase in hornblende at the expense of grunerite, more
siliceous character and the presence of significant quantities of
gold.  Sulphide minerals include, in decreasing order of abundance,
pyrite, pyrrhotite, chalcopyrite, arsenopyrite, loellingite and
sphalerite. Arsenopyrite is rare in
contrast
with other iron formation-hosted gold deposits in the Slave
Province.  Significant levels of gold are present in a number of
discrete zones in the Bugow iron formation, including the Cabin
Lake, Andrew South, Andrew North, Camp, Beaver and Twilight zones.
All zones are located along fold limbs despite higher levels of
sulphides in fold noses. Gold occurs in association with sulphides
although in detail, it is not found within sulphide grains. It is
most common as 10-20 micron grains interstitial to silicates and at
the boundary between quartz veins and chlorite-hornblende-rich iron
formation. Less common sites include fractures near quartz veins
and as inclusions in rare arsenopyrite and in pyrite.  The Cabin
Lake zone has received the most exploration attention to date.
Erratic, high grade drill intersections are concentrated in an area
about 100 m long, 60 m deep and 12 m wide. Although the zone is
stratabound, it transgresses the Bugow iron formation internally,
crossing from a location near the base of the unit to one near the
top. A reserve of 70,000 tonnes grading 10.29 g/t Au is reported in
DIAND Mineral Industry Report 1986-87. Aber Resources  1987 Annual
Report states a figure of 100,000 tons grading 0.3 oz/ton Au.
The Andrew zones are reported to contain 43,900 tonnes grading 4.46
g/t Au (Bugow or Andrew South) and 18,100 tonnes grading 7.89 g/t
Au (Andrew North, #085OSW0040) (Canadian Deposits Not Being Mined
1989).  The Bugow Showing ( Andrew South) has two satellite
showings. One to the north is the Andrew North Showing (NORMIN
Showing Number 085OSW0040) and the other to the south is the AH 205
(# 085OSW0041). Both of these showings are within the same iron
formation unit that hosts the Bugow Showing.  North of the Cabin
Lake Showing and along strike are, from south to north, the Beaver
Showing (085OSW0043), the Camp Showing (085OSW0044) and the Camp
North Showing (085OSW0045). All of these showings are within the
same iron formation unit that hosts the Cabin Lake Showing.
The Bugow claim group has had trenching, sampling, detailed mapping,
diamond drilling of the key showings and both ground and airborne
geophysics. The ground and airborne geophysics done include
magnetetometer, electromagnetics and induced polarization.
Regional The area is within the Slave Structural Province and lies
near the south end of the Russell Lake-Slemon Lake Supracrustal
belt. This supracrustal belt comprises Archean metavolcanics and
metasediments of the Yellowknife Supergroup.  The Russell Lake area
is largely underlain by greywacke-mudstone metaturbidites and
lesser amounts of felsic and mafic metavolcanics. Felsic
metavolcanics are exposed along the eastern shore of Russell Lake
in a southwest trending belt. Mafic metavolcanics occur five
kilometres west of Russell Lake in two narrow southwest trending
belts and as a narrow southwest trending belt at Mosher Lake, some
10 kilometres east of Russell Lake. Later Archean granitoid
intrussions cut the supracrustal sequences. These consist of
tonalitic to granitic plutons to the northwest, northeast and south.
Numerous small granitic plugs are exposed throughout the Russell
Lake area.  The strike of the metasediments is generally northeast
with some wrapping of the metasediments around a granitic plug near
Murkey Bay on Russell Lake. The metasediments are isoclinally
folded about northeast trending anticlinal and synclinal axes with
preferential overturning to the west. The fine grained
metasedimentary unit which hosts silicate and minor sulphide facies
iron formation is repeated across Russell Lake between the
metavolcanic rocks to the east and west.
Property The property is underlain by a narrow belt of volcanic
rocks of the Yellowknife Supergroup that strike N-NE through Mosher
Lake. On both sides greywacke and slate rocks bound the volcanics
which are light to dark green andesite and basalts and massive
schistose and pillowed flows. At the contacts they are interbedded
with white-weathering porphyritic rhyolite and schistose tuff,
agglomerate and breccia.  The slightly altered sedimentary rocks
are interbedded slates, arkoses, quartzites and phyllites. The
greywackes are dark grey and sandy textured and weather to a dark
grey, greenish or buff colour. The sediments lie in a series of
tight isoclinal folds with steep dipping or overturned axial planes.
The volcanics also dip steeply but the folds seem to be broader.
Showing The showing strikes northeasterly and lies between
schistose and massive basic flows in a rusty mineralized zone. The
zone can be traced for 1,200 feet and carries massive, fine-grained,
schistose amphibolite mineralized with pyrrhotite, pyrite, and
arsenopyrite. Quartz stringers parallel the schistosity in
irregular lenses and veins and also crosscut in gash veins.  The
south end of the mineralized zone is terminated by tourmaline
pegmatites. A fault, filled by diabase, offsets the centre of the
zone 50 feet.
The gold assays from trenching on the north section returned values
from trace to 0.49 oz/ton over 6 feet. Diamond drilling returned
gold assays from trace to 0.70 oz/ton over 5 feet. The zone
averages 0.15 oz/ton gold over 25 feet for 300 feet based on
surface trenching. The zone averages 0.07 oz/ton across 58 feet
based on diamond drilling for the full strike length of 1200 feet.
Drill indicated reserves to a depth of 170 feet is 552,000 tons
grading 0.082 oz/ton gold.  Exploration This showing has had
trenching and diamond drilling done. A resource has been calculated
based on this information. Drill indicated reserves to a depth of
170 feet is 552,000 tons grading 0.082 oz/ton gold.
intrusions cut the supracrustal sequences. These consist of
Property/Showing Significant levels of gold are present in a number
of discrete zones in the Bugow iron formation, including the Cabin
top. A reserve of 70,000 tonnes grading 10.29 g Au/t is reported in
Report states a figure of 100,000 tons grading 0.3 oz/ton Au.  An
Aber Resources Ltd. press release dated 1986/08/18 summarizes the
assay results from the first four diamond drill holes from the
Cabin Zone. Hole A86-1 averaged 0.35 oz/ton Au across 29 feet, hole
A86-2 averaged 0.24 oz/ton Au across 16 feet, hole A86-3 averaged 0.
46 oz/ton Au across 26.3 feet and A86-4 averaged 0.23 oz/ton Au
across 5.0 feet, 0.20 oz/ton Au across 10.0 feet and 0.46 oz/ton Au
across 20.0 feet.
Work on the Bugow claim group includes trenching, sampling,
detailed mapping, diamond drilling of the key showings and both
ground and airborne geophysics. The ground and airborne geophysics
done include magnetometer, electromagnetics and induced
polarization.
The Nicholas Lake vein gold deposit is located near the northern
end of the Yellowknife Basin, a supracrustal belt within the
Archean Slave structural province. Turbiditic metasediments of the
Burwash Formation, part of the Yellowknife Supergroup, have been
intruded by pink granite and a medium to coarse-grained
granodiorite which is the host for mineralization. Numerous dykes
and irregular masses of granodiorite are present in an area
extending southwest of the main granodiorite intrusion. The
metasediments have been deformed into tight folds with bedding now
generally striking northwesterly with a steep dip. A strong,
parallel to subparallel axial plane foliation is superimposed on
the stratified rocks. Regional metamorphic grade is lower
amphibolite facies.  The Nicholas Lake deposit comprises a series
of essentially vertical quartz-sulphide veins in a subvertical to
vertical, altered granodiorite stock about 200 m in diameter
intruding metasediments. Intense shearing, sericitization and
silicification are common, particularly along the southern contact.
At least three varieties of quartz have been recognized and
multiple episodes of brecciation and rehealing are evident. The
best veins and gold values are concentrated along the southern
altered border zone and are restricted to the granodiorite.  Higher
grade gold values are associated with massive, fine-grained
pyrrhotite coating angular fragments of arsenopyrite and quartz,
massive arsenopyrite and pyrite with lesser sphalerite and galena,
vein quartz with visible gold and coarse-grained sphalerite and
galena, and quartz veins with pyrite. Some gold is present in
association with disseminated sphalerite and minor quartz veinlets
within zones of brecciated and fractured granodiorite.
Sulphides may also occur as massive lenses up to 65 cm wide.  The
deposit has been traced by drilling over a strike length of 200 m
and to a depth of about 300 m. A reserve (indicated and inferred)
of 1,114,600  tonnes grading 12.16 g Au/t has been calculated using
a cutoff grade of 5.0 g Au/t. Metallurgical tests established that
94% of the gold could be recovered using a 60% minus 200 mesh grind
and flotation of sulphides followed by a regrind to 90% minus 350
mesh and cyanidization.
Gold mineralization occurs in short, narrow quartz veins cutting
fragmented Archean amphibole gneiss of the Yellowknife Supergroup.
Diamond drill intersected gold bearing veins at 400 and 800 feet
gave a reported average grade of 0.3 oz/t in the main zone. A
resource of 100,000 tons at 0.62 oz/t is listed.  Sporatic
exploration was done from 1944-56 and included trenching,
geological mapping, sampling and diamond drilling. In 1981 Newmont
Exploration Canada optioned the property and subjected the showing
to geological mapping, sampling, geophysical surveys of magnetics,
EM, IP and diamond drilling.
In the Cross Lake showing visible gold is associated with sulphides
in quartz veins within a shear zone cutting a knotted quartz mica
schist derived from impure greywacke and slate of the Archean
Yellowknife Supergroup.  A diamond drill indicated resource was
listed 30,000 tons at 0.31 oz/
t
Visible gold in discontinuous quartz veins in greywacke of the
Archean Yellowknife Supergroup. This showing has been subjected to
sporatic exploration since the 1940s including, pitting, trenching
and diamond drilling. A diamond drill indicated resouerce of 4,400
tons at 0.47 oz/t is listed.
The Kim prospect (Main Zone) is located in the Indin Lake
supracrustal belt, part of the Archean Slave structural province.
The belt consists of irregular, generally north-trending belts of
Archean Yellowknife Supergroup rocks, including mainly basaltic
volcanic rocks, turbiditic greywackes and mudstones dated at 2669 +/
- 15 Ma. Intervening areas are made up of hybrid rocks derived from
both basement granitoid and supracrustal rocks as well as plutonic
rocks, generally granite or granodiorite.  Detailed mapping by Echo
Bay Mines has identified the following stratigraphy in the area of
the deposit: a basal sequence of pillowed and massive basalts and
irregular gabbroic bodies overlain by the lower massive basalt, a
lower amygdaloidal pillow unit characterised by carbonate amygdules,
an upper massive basalt and finally an upper amygdaloidal pillow
unit characterised by quartz-feldspar amygdules. The volcanic
package has been metamorphosed to amphibolite facies, but is in
fault contact with a package of turbidites which are at lower
greenschist facies. This vertical ductile fault represents a major
break in the area, which is structurally complex. Sedimentary rocks
are isoclinally folded and broader folding is recognised within the
volcanics. Northwest-trending left-lateral strike-slip faults with
near vertical dips, are the latest and predominant faults in the
area.  The Main Zone on Lex Lake is a stratabound deposit,
consisting of quartz-carbonate veins in fractured, sulphide-rich,
silicified massive basalt flows about 60 metres from their contact
with the sediments. It strikes northerly and dips steeply to the
west. An early white quartz vein set is cut by a later smoky quartz-
carbonate set with which the gold is associated.
Veins are deformed and show strong ribbon textures along their
contacts. Both arsenopyrite and pyrrhotite are found within the
veins and in haloes extending 20 to 30 cm from them. Pyrrhotite
crystals are aligned along a prominent and steeply plunging
stretching lineation commonly developed in basalts in the immediate
area of the deposit. Arsenopyrite is generally massive to euhedral,
overgrows and possibly replaces pyrrhotite and is commonly brittley
deformed along the stretching lineation. Free gold, in places
visible, is found in quartz-carbonate veins, in fractures cutting
arsenopyrite crystals and in sulphide-rich haloes adjacent to veins.
Total drilling on the Main zone in the period 1984-1990 was 13,
607.5 metres. Mineralization has been intersected over a strike
length of 731 metres and has an average width of 4.6 metres. The
zone has been divided by faulting into six blocks. In 1987, a
reserve totalling 112,500 tonnes grading 7.89 g Au/t was calculated
for one block containing about 10% of the total tonnage. The cutoff
grade used was 4.00 g Au/t and minimum width 1.5 metres. Four deep
drill holes have confirmed the depth extension of mineralization to
365 metres and the deposit remains open at depth. A three tonne
bulk surface sample was collected for metallurgical and
conductivity sorting tests.
The Cass prospect is located in the Indin Lake supracrustal belt,
within the Archean Slave structural province. The belt consists of
irregular, generally north-trending belts of Archean Yellowknife
Supergroup rocks, including mainly basaltic volcanic rocks,
turbiditic greywackes and mudstones dated at 2669 +/- 15 Ma.
Intervening areas are made up of hybrid rocks derived from both
basement granitoid and supracrustal rocks as well as plutonic rocks,
generally granite or granodiorite.  The Cass zone is located about
3 km southwest of the Main zone constituting the Kim prospect. Gold
occurs in steeply dipping quartz-carbonate veins cutting and
restricted to a northeast-trending, subvolcanic gabbroic sill which
intrudes a sequence of intermediate to felsic flows and
pyroclastics. The gabbro varies in width from 20 to 100 m and has a
strike length of approximately 2 km.  Mineralization is associated
with two sets of smoky-white, mottled  quartz and quartz-carbonate
veins up to several metres long and up to 0.5 m wide. The less
abundant quartz-rich set is sub-parallel to regional foliation
while the quartz-carbonate set cuts it at 70-80 degrees and is
oriented at a high angle relative to the gabbro contacts. Several
layers of carbonate and quartz are present in each vein, with
carbonate tending to occur in the central portions. The veins are
folded about steeply plunging axes, both in a gross sense involving
the entire vein and internally. Grunerite-garnet veins with diffuse
contacts extend outward from the quartz-carbonate veins and form
selvages around them. Garnet is also present in haloes around the
veins.
Arsenopyrite occurs in diffuse zones of coarse-grained euhedral
crystals adjacent to veins in the silicified metagabbro and as
anhedral crystal masses within the veins and along vein contacts.
Pyrrhotite is most abundant in haloes 30 - 50 cm wide adjacent to
veins but is also disseminated throughout the sill. Pyrite is found
as cubes and irregular aggregates. Gold occurs within sulphides and
as native metal concentrated along the contacts of the quartz-
carbonate veins. Both arsenopyrite and pyrrhotite have been
deformed, the former fractured and brittly boudinaged along a
regional lineation, the latter elongated parallel to it.  Drilling
in the period between 1984 and 1990 totalled 10,479 m. The Cass
zone has been traced by drilling over a strike length of 300 m, to
a depth of 210 m and is open to the southwest. It ranges between 1
and 15 m in thickness, averaging 4.9 m. A probable reserve on a 120
m long by 210 m deep block has been calculated at 336,300 tonnes
grading 7.17 g Au/t. A three tonne bulk surface sample was
collected for metallurgical and conductivity sorting tests.
Mineralization withion a series of conformable auriferous quartz
veins, stringers and lenses hosted by by N-NNE striking greywackes,
slates and volcanics of the Archean Yellowknife Supergroup. The No.
1 vein mineralogy consists of quartz-pyrite-arsenopyrite,
pyrrhotite, chalcopyrite and visible gold. A resource of 29,000
tons at 0.35 oz/t has been calculated.  Work on the showing
includes trenching, diamond drilling, geochemical sampling and
geological mapping.
Galena, sphalerite, arsenoipyrite, chalcopyrite and gold
mineralization occurs in a 100 foot wide belt of argillite-quartz
veining in siltstone-shale unit within the Proterozoic Snare Group.
A 5x8 foot wide mineralized zone plunges 45 degrees below the lake
to a depth of 300 feet below the lake. Exploration on this showing
include trenching, geological mapping and sampling, diamond
drilling, EM geophysical surveys and a petrographic study. A
diamond drill inferred resource of 81,000 T at 0.228 oz/t gold
(uncut) is listed.
In this showing gold is found in sediments of the Yellowknife
Supergroup at or near the conbtact with volcanics. Aurioferous
zones are generally silicified, probably due to the intrusion of
the 6-12 m wide Gamble Dyke, an albite-porphyritic ENE trending
dyke. Work done on the showing includes trenching, geological
sampling, diamond drilling, geological mapping, soil sampling and
geophysical magnetic and EM surveys. Resources calculated are
probable at 116,185 tons at 0.411 oz/t gold (diluted) plus 33,972
tons at 0.128 oz/t gold.
Zones of auriferous quartz veins and stringers are offset by NNW
trending faults in schistose greywackes and argillites of the
Archean Yellowknife Supergroup. Metallic minerals comprise
approximately 1% of the vein material and include pyrite-
arsenopyrite-pyrrhotite-galena-chalcopyrite-sphalerite and
jamesonite and free gold.A resource of 72,500 tons at 0.36 oz/t
gold is listed.  Work done on the showing includes: 1945-49:
trenching, diamond drilling, sinking a shaft to the 525 foot level
(3 levels, 1979-82: shaft rehabilitation and dewatering, 1988:
diamond drilling.
Two zones, the Main and the A make up this showing. The Main zone
comprises a gold bearing stockwork of quartz veinlets in
aconformable graphitic shear in sediments of the Archean
Yellowknife Supergroup. Outside the Main shear, gold occurrences
are associated with conformable quartz veins in volcanics. A shaft
was sunk to 525 feet and lateral work explored the A zone on the
175 foot level and the Main zone on the 300 foot level.  Resources
calculated: A zone = 23,000 tons diamond drill indicated at 0.54 oz/
t (1948); Main zone = 600x5 at 0.44 oz/t gold to depths of 160 feet
to 300 feet. A 1980 reevaluation of unspecified North Inca
deposit(s) produced an estimate of 90,000 tons at 0.20 oz/t gold.
The Indin Lake area is situated in the southwestern portion of the
Slave Structural Province near the contact with the Bear Structural
Province (Wopmay Oregon).  It is underlain by Archean age rocks
which are part of the Yellowknife Supergroup and are comprised of
volcanic and sedimentary strata forming a north-northeast trending
supracrustal belt. This irregular shaped belt extends south
approximately from the south side of Truce Lake to the southern
portion of the Snare River.  The Indin Lake Supracrustal Belt is
bounded to the west by Archean granitoid plutons and migmatites
while gneissic rocks flank the eastern side and are thought to be
basement rocks to the belt.  All the rocks within the belt are
strongly folded and there is a  complicated deformation history
associated with the area.    Volcanic rocks of the Indin Lake area
occur as mafic, intermediate and felsic units.  Mafic lithologies
dominate the volcanic suite of rocks, which include pillowed flows
(minor andesite) and local interflow breccias. Intermediate rocks
include volcaniclastic units (mainly breccias) occurring usually as
lens shaped bodies and may dominate the lithology within small
isolated portions of the belt (eg. Leta Arm and Spanner Lake areas)
.  Ocurrences of quartz diorite and gabbro sills, scattered
throughout the Indin Lake Belt, are thought to be related to the
volcanic units in the area .  One of these sills adjacent to Baton
Lake is an albitic and auriferous intrusive within a mafic volcanic
package and hosts the Colomac Mine deposit (showing I.D. No.
086BSW0004 and reference I.D. No. 1994-Cp91).
Sediments in the area comprises turbiditic greywackes and mudstones.
Hosted within the sediments in the eastern portion of the Indin
Lake Belt are strongly folded banded iron formation units
consisting of  five main facies: silicate-oxide facies, silicate-
amphibolite facies, silicate-sulphide facies, silicate-chlorite
facies and cherty exhalitive facies.  These iron formation units
occur as lens/pods or conformable beds that may be traced out for
several kilometres with widths up to 10s of metres and are locally
auriferous.  Quartz veins (locally auriferous) often cut the
exhalitive and turbiditic units, with increased concentrations in
the area of the fold noses (reference I.D. No. 1994-Cp91 and
083396).  Granodiorites and pegmatites intrude the belt and
generally cut the volcanic and turbidite rocks with variable
emplacement ages.  Possible synvolcanic emplacement has been
obsereved locally within the area.  The Cotterrill Lake complex
(hornblende - biotite granodiorite/hornblende monzogranite) is
basement rock within the belt.  Diabase (to gabbro) dyke swarms
occur throughout the Indin Lake area and cut all pre-existing rock
units.   Evidence of four deformational events was observed by
Pehrsson and Beaumont-Smith (reference I.D. No. 1994-Cp91) while
preforming mapping in the Indin Lake Supracrustal Belt.  All the
rocks in the belt have been metamorphosed to lower greenschist to
amphibolitic facies.
The Horseshoe Zone is described as a banded iron formation hosted
within a greywacke-argillite package all of Archean age.  The zone
is situated within a synclinal fold structure with the main
mineralization occuring at the closure, extending into the limbs of
the fold.  Drilling has indicated that gold is concentrated in
layers through the iron formation.  A strike length of at least 1,
000 feet has been intersected during the exploration surface
drilling.  Information on the showing is available only from news
releases where only limited details are given.
The Horseshoe Zone is located along the southern shore of Damoti
Lake and is associated with several other banded iron formation
gold showings in the vicinity.  The Horseshoe Zone has two other
smaller zones (Pyrite Zone and Red Mountain Zone) directly adjacent
to it and can be considered all part of one zone.  The zone was
first discovered in a 1993 exploration programme which included
bedrock sampling and mapping at a 1:2000 scale, over the southern
portion of the Damoti Lake property.  One grab sample described as
a medium grained amphibolite with thin pyrite stringers assayed 1.
41 g/t gold. Additional work (1994 to 1998) included surface
exploration drilling and an underground decline into the zone in
order to better delineate the mineralization.  Mineralized iron
formation (4000 tons) was mined from 2 exploration drifts and
stocked piled for future processing.  A  few underground
exploration diamond drill holes were completed to aide in
delineating the extent of gold mineralization.  More than 35
surface diamond drill holes have been drilled into the Horseshoe
Zone todate with very significant results including 12.143 feet at
4.380 oz/ton gold (D94-113) and 10.50 feet of 0.680 oz/ton gold
(D97-307).  Reserve calculations were completed on the zone
resulting in a demonstrated reserve figure of 212,350 ounces of
gold  and an inferred resource of 148,178 ounces of gold.
Numerous occurrences, generally high grade pitchblende pods of
restricted spatial extent. Numerous of these have been examined by
drilling, open pits, or underground work including drifting and
raising. No. 3 and No. 4 as sampled underground on three
consecutive raise faces yielded an average of 0.678% U3O8 across 3.
88 ft for a raise length of 16 ft. A combined 1.5 tons of ore
assaying 40.5% U3O8, taken mostly from pits on No. 3 and No. 4, is
said to have basically cleaned out those two showings; however, two
lenses in the No. 3 and No. 4 area are also said to contain an
estimated 200 tons grading 3% U3O8. 1970s drilling could find no
extensions to these lenses.
Undg dvlp outlined ore zone of 300 by 1.5 ft with 0.35% U3O8.
The Izok Lake deposit lies within the Point Lake Volcanic Belt, a
north trending belt of Archean mafic to felsic volcanics and
subordinate sediments which have been subjected to polyphase
Archean deformation and regional metamorphism. The deposit is
beneath Izok Lake, in the Izok sub-belt, a NE to north trending arm
of volcanic supracrustals which juts from the east side of the
Point Lake Belt just north of Itchen Lake. The rocks in these belts
belong to the Point Lake Formation of the Yellowknife Supergroup.
Itchen and Contwoyto Formation metaturbidites, also of the
Yellowknife Supergroup, overlie the Point Lake Fm and are exposed
about 2 km SE of Izok. 2 km SW of Izok, a sedimentary-felsic
volcanic sequence is now exposed as siliceous gneisses. Within a
kilometre north and east of Izok, a mixed sedimentary-volcanic
sequence correlative with Yellowknife Supergroup rocks, is intruded
by numerous, late Archean granitic sheets, creating lit-par-lit
gneisses. The granitic bodies coalesce into the Rockinghorse
Batholith about 2 km NE of Izok.  The deposit is hosted near the
top of a thick felsic pile, by rhyolitic and dacitic flows and
tuffs metamorphosed to felsic gneisses. It is conformably underlain
by similar rocks, and toward the edges of the Central Zone is
underlain by rhyolite agglomerate. It is conformably overlain by
felsic flows and tuffs, and near the felsic centre by a pyritic
muscovite schist, perhaps derived from a cherty tuff. Minor mafic
gneisses in the hangingwall are probably derived from intermediate
to mafic tuffs. An amphibolite unconformably overlies the host
felsic volcanics, and three bodies of amphibolitic metagabbro
intrusive into the volcanics outcrop around Izok Lake.
Massive to pillowed, mafic to intermediate flows overlie the felsic
pile. A late Archean, tourmaline granite-pegmatite cutting the
deposit is locally Pb-enriched.  The deposit consists of the North
and Central Zones, initially described separately but recently
discussed as one; the Northwest Zone; and the recently discovered
Inukshuk Zone. The Central-North Zones form a trough-shaped, flat-
lying, composite lens of massive sulphides measuring 450 by 110 m
horizontally. Its long axis trends ENE and plunges 15-30 degrees
ENE. It has a highly variable thickness, from 0 - 160 m deep. A Cu-
rich stringer zone under the west end of the Central Zone is south
dipping, about 100 m long x 20 m deep, at a depth of 100 - 160 m
from surface.  The Northwest Zone, centred about 250 m NW of the
Central Zone, is a fairly flat-lying lens, somewhat concave upwards
and dipping shallowly north. Its surface lies at 30 - 130 m depth
and it measures 200 by 280 m horizontally and 22 m vertically. Both
the Central and the Northwest Zones are open-pit prospects with a
stripping ratio of 3:1. The Inukshuk Zone, discovered in 1992 400 m
east of the main deposit, is an elongate, ENE-trending lens dipping
shallowly south. It measures greater than 300 m long by 150 m by 10
m thick, at 60 - 400 m depths. It partly underlies Izok Lake and,
unlike the main deposit, is an underground mining prospect.  The
main deposit (Central and Northwest Zones) lies in NE-trending and
plunging, synclinal folds. The variable thicknesses of the sulphide
layers is interpreted to be partly an original depositional feature,
which may have localized fold axes, and partly due to
deformational boudinaging and necking.  Sulphides are coarse
grained and massive, comprised of mainly sphalerite, chalcopyrite,
pyrite and pyrrhotite.
Zoning in the Central Zone, above the Cu-rich stringer zone,
consists of a massive, Cu-rich basal section overlain by a Zn-rich
section, itself locally overlain by a Zn-Pb-rich section. There is
considerable evidence for re-mobilization of galena and
chalcopyrite during deformation and/or metamorphism, and this
apparently has disrupted more subtle zonations.  Sericite-biotite
alteration is pervasive in an envelope around the deposit,
silicification is less extensive and intensive, and minor
aluminosilicate alteration has been noted. A Mg-enriched, chlorite-
cordierite-anthophyllite rock underlies a marked thinning of the
Central Zone and is interpreted to represent a conduit for
upwelling hydrothermal solutions through a volcanic cone or ridge.
Reserves were estimated in 1992 at 2 million tonnes of 2% Cu and 8%
Zn, inferred, for the Inukshuk Zone, open down-plunge. Also in 1992,
the main deposit was estimated, on the basis of 148 DDH on 60 m
centres, to have probable and possible reserves of 12.0 million
tonnes grading 31.% Cu, 1.4% Pb, 14.5% Zn and 74.8 g/t Ag, and
inferred reserves of 1.4 million tonnes grading 3.8% Cu, .8% Pb, 13.
1% Zn and 66.5 g/t Ag.
The showing is in the Contwoyto - Itchen - Point Sedimentary
of the Yellowknife Supergroup. It is flanked 5 km to the west by
the older, predominantly volcanic Point Lake supracrustal belt, and
invaded to the east by late Archean granitoids. Late Proterozoic
diabase dykes cut all other lithologies.  The Contwoyto Formation
sediments underlying the showing area consist of schistose
argillites with subordinate greywacke and interbedded lenses and
layers of iron formation. These strike N and dip 50E to vertically.
A cordierite isograd marking a transition to lower amphibolite
facies is immediately east of the showing.  The showing is a zone
of iron formation and interbedded black, fine grained, graded-
bedded argillite locally grading into greywacke. The iron formation,
in 3 and locally 4 discrete members, is folded and overall N-
striking and almost vertical. It a garnet-amphibole iron formation
with abundant cross-cutting and conformable quartz veins, and
conformable sulphide layers made up of disseminated pyrrhotite,
arsenopyrite, and pyrite. The host unit has been traced by exposure
and geophysical response for 700-800 m, the northernmost 490 m of
which is overburden-covered. At least 100 m and probably 350 m of
its strike length has been systematically drill-tested. It averages
3.5 m thick at surface but ranges between 10 and 35 m thick to
depths of 300 m. Gold appears to be evenly distributed throughout
and the potential exists for 2 to 3 million tons grading 0.29 oz/
ton (George Cross Newsletter, 1989 No.235 & 1990 No.89 & 179).
The Takijuq-Hood deposits lie in the northern Slave Province, in
the Takijuq Lake-Hood River Supracrustal Belt, a 125 km long, NNE-
trending belt of Archean Yellowknife Supergroup mafic to felsic
volcanics and various intrusives into them. At its north end, the
Belt is only a few kilometres south of the southern end of the
Anialik River Supracrustal Belt, and its south end apparently
adjoins the north end of the Point Lake Belt (EGS 1992-16). Near
its south end, at the south end of Takijuq Lake, the belt widens
into an ENE-trending segment 8 km long and 1.5 km wide. This
Takijuq South Segment hosts the Takijuq-Hood deposits and showings.
The Segment contains a greater proportion of felsics than the rest
of the belt. The felsics are under and overlain by intermediate to
mafic volcanics, and all are intruded by common, subconformable,
gabbro and porphyritic gabbro bodies. The felsics are thought to
represent a volcanic centre. North of it, a highly deformed,
gabbroic to tonalitic complex cut by mafic and ultramafic dykes is
thought to be pre-Yellowknife Supergroup (EGS 1992-16). All these
earlier Archean rock types are invaded along the north and south
edges of the Segment by mixed, diorite/gabbro plutonic complexes.
These in turn are cut by granitic dykes related to late Archean
granitoid plutons which flank the Segment to the north and south
and pinch it off to the NE.  To the west, a NNE-trending fault
brought a wedge of fine clastic metasediments, of uncertain
stratigraphic postition within the Yellowknife Supergroup, into
contact with the volcanics. The wedge or belt is less than 1 km
across, it s eastern limit defined by late Archean plutonic rocks.
Proterozoic diabase dykes of 2 generations cut all other
lithologies. The most abundant are NNW to NW-trending dykes of the
Mackenzie swarm.  The Takijuq H-41, or Hood 41, deposit is in an
area of predominantly mafic volcanic rocks south of the felsic
centre, invaded by both mixed plutonic rocks and late granitic
rocks. The deposit is hosted by andesites and to a lesser extent by
felsics, and follows the contorted, NNE-trending contact between
them. The felsics form a wedge between the host andesitic unit to
the NW and a major unit of amygdaloidal andesite to the SE (thought
to be stratigraphically below). A granitic intrusive body (late
Archean?) cuts off the NE end of the felsic wedge and the sulphide
zone, and granitic rocks of a mixed diorite/gabbro plutonic complex
are exposed 60m west of the deposit and cut it off to the SW at
depth.  Regionally, the deposit is far out on the SE limb of a SW-
plunging, macro-syncline whose axial plane strikes NE and dips
steeply SE.  Regional metamorphism to lower greenschist grade has
been overprinted by contact metamorphism to lower amphibolite grade.
The host massive and pillowed andesites are now well-foliated and
chloritic. The host felsics are now mica-chlorite-sericite-quartz
schists, locally exhibiting chlorite and sericite bands (possible
remnant tuffaceous banding), and rarely hosting sericitized
fragments. Massive magnetite at the contact between granitic rocks
of the complex and the sulphide layer is thought to derive from a
contact metamorphic reaction in the sulphide layer.  The sulphides
are massive at the NE end and stringer to massive at the SW, in a
layer at least 120 m long and 25 m wide, and intersected to 200 m
down-dip.
Surface exposure is a 61 x 15 m gossan which yielded chip samples
assaying up to 4% Cu and 10% Zn, and grabs up to 6% Cu, 5% Zn and
144 g/t Ag. Drilling in 1975 cut slightly lower grades over 8 to 38
m widths. Subsequent drill results were not reported but in 1991
Minnova announced reserves in two zones, 900,000 tonnes in Zone 41
grading 3.2% Zn, 1.4% Cu and 12 g/t Ag, and 1,100,000 tonnes in
Zone 41A grading 3.3% Zn, 2.4% Cu and 16 g/t Ag.
Belt is only a few kilometres from the southern end of the Anialik
River Supracrustal Belt, and its south end apparently adjoins the
north end of the Point Lake Belt (EGS 1992-16). Near its south end,
at Takijuq Lake, the belt widens into an ENE-trending segment 8 km
long and 1.5 km wide. This Takijuq South Segment hosts the Takijuq-
Hood deposits and showings.  The Segment contains a greater
proportion of felsics than the rest of the belt. The felsics are
under and overlain by intermediate to mafic volcanics, and all are
intruded by common, subconformable, gabbro and porphyritic gabbro
bodies. The felsics are thought to represent a volcanic centre.
North of them, a highly deformed, gabbroic to tonalitic complex cut
by mafic and ultramafic dykes is thought to be pre-Yellowknife
Supergroup (EGS 1992-16). All these earlier Archean rock types are
invaded along the north and south margins of the Segment by mixed
diorite/gabbro plutonic complexes. These in turn are cut by
granitic dykes related to late Archean granitoid plutons which
flank the Segment to the north and south and pinch it off to the
northeast.  To the west, a NNE-trending fault zone and cross-faults
have brought wedges of fine clastic metasediments, of uncertain
stratigraphic position within the Yellowknife Supergroup, and
blocks of late Archean plutonic rocks into contact with the
volcanics.  Proterozoic diabase dykes of two generations cut all
other lithologies.
The most abundant are NNW to NW-trending dykes of the Mackenzie
swarm.  The Takijuq H-10, or Hood 10, deposit is in the felsic dome.
This consists mainly of massive to well-foliated quartz-eye
rhyolite, rhyolite agglomerate, rhyolite tuff and dacite.
Regionally the felsics are underlain by mafic flows and tuffs with
intercalated carbonate beds, and overlain by laterally extensive,
pillowed and massive mafic flows and tuffs. The felsics are
restricted in areal extent and may represent the explosive end
stage of the first of two cycles of volcanism in the Takijuq Belt
(Gill 1976).  A narrow, mafic to ultramafic dyke which is
calcareous, chlorite-rich and locally serpentinized, cuts the H-10
deposit in the vicinity of DDH H-10-5, trending 040 - 050 degrees
(parallel to the main penetrative foliation).  Late Archean
granitic rocks are in intrusive contact with the felsic volcanics
150 m south of the deposit, and in NW-trending fault contact with
them 150 m west of the deposit. Emplacement of these plutonic rocks
was preceded by at least two phases of deformation, the first
producing a major syncline, the second only minor folds, and lower
greenschist facies regional metamorphism, and was accompanied by
contact metamorphism which raised the grade of nearby rocks,
including the deposit, to lower amphibolite.  A number of 1 - 2 m
wide Proterozoic diabase dykes cut the deposit area.  The main
deposit consists of four separate, possibly en echelon, pencil-
shaped lenses of massive sulphides, possibly representing four
separate mineralizing events. The lenses plunge NNE at 60 degrees,
and the deposit as a whole is about 270 m long, on average
approximately 12 m but up to 70 m wide, and about 250 m deep, based
on information to 1976.
It strikes SE, dips subvertically NE, and probably faces NE,
although other lithological contacts in the vicinity strike east.
Exposure is poor and structural interpretation was preliminary and
inadequate in the latest available reports (1976), which suggest
that the deposit lies on the SE limb of a major NE-trending
syncline affected by minor north trending folds.  The sulphides are
hosted mainly by a laterally extensive unit of amygdaloidal
andesite, over and underlain by cherty rhyolite which is a
subordinate host. Chloritic alteration is locally heavy, especially
to the north. A well-defined alteration pipe is absent (Gill 1976),
although stringer sulphides to the west underlie the massive,
banded and non-banded zone. The sulphide lenses comprise massive to
disseminated to stringer pyrrhotite-chalcopyrite-pyrite-sphalerite-
(galena)-(marcasite), with clear mineralogical and metal zoning
indicating Cu-rich zones underlying Zn-rich zones. A hundred and
fifty metres north of the main H-10 zone is a second sulphide
deposit, relatively Pb-Zn rich and known as the 10b zone. It is
characterized by pyrite-pyrrhotite-sphalerite-galena as amygdule
cores and partial infillings.  Grabs assaying up to 0.51% Cu, 2.1%
Pb, 12% Zn and 48 g/t Ag stimulated interest in the showing. Later
drill intersections assayed as much as 8% Cu, 2.7% Pb, 19% Zn, 65 g/
t Ag and 4 g/t Au over 1 m to 16 m core lengths, and selected 1991
drill intersections are 5.7% Cu and 5.1% Zn over 46 m, and 3.5% Cu
and 3.3% Zn over 36 m.  A 1991 estimate of drill-indicated reserves
is 1.2 million tonnes grading 4.1% Cu, 4.4% Zn and 27 g/t Ag
(Minnova Inc, Toronto, Press Release, Nov 29/91).
Bornite, chalcopyrite, pyrite, hematite and carbonate found in vugs,
fractures and vein breccia in 2 quartz stockworks cutting dacite
of the Aphebian Cameron Bay Group.  Work done on the showing
includes: 1921: discovery 1950-57: test pitting, sampling, diamond
drilling (in 1957, 3,473 feet of widely spaced diamond drilling was
done) 1968-69: geological mapping, prospecting, trenching,
radiometric, EM and magnetic surveys were done. Diamond drill
inferred resources are listed as 100,000 tons at 8.4% copper to 275
feet.
Chalcocite and malachite occur in a brecciated shear zone in
basalts of the Neohelikian Copper Creek Formation - Coppermine
River Group. The showing area was worked from 1967-68 and included
prospecting, geological mapping, geophysical surveys and diamond
drilling. Drilling indicated a deposit having the dimensions of 107
m x 1.2 m x 46 m deep with an estimated resource calculated at 125,
000 tons at 2% copper to a 600 foot depth.
Chalcocite and bornite occur as narrow veinlets in fault hosted
quartz veins that crosscut brecciated basalts of the Coppermine
River Group.  From 1967-69 the showing was subjected to prospecting,
geological mapping, IP survey and 22 diamond drill holes. A
tonnage and grade of 131,000 tons at 2.89% copper (1968) was based
on 8 drill holes totalling 840 feet.
Mineralization occurs as a tabular body (1,500 feet long x 35 feet
wide) containing chalcocite and some bornite in a fractured and
shattered zone along a fault cutting basaltic flowss of the
Neohelikian Coppermine River Group.  Work done on the showing
includes: 1967-68: EM, IP and magnetic surveys, geological mapping,
diamond drilling, airfield and tote road building, milling tests
(60% copper concentrate with 4 to 5 oz/t silver and 92% copper
recovery). 1971-72: gerochemical work 1981: results of the
geochemical work under study  Resources calculated are listed as 4,
162,000 tons at 2.96% copper, 10% dilution. The estimated tonnage
is to 600 feet, open at depth and along strike to the SW.
Mineralization consists of chalcocite, minor bornite, chalcopyrite
and pyrite in a highly fractured/brecciated basalt of the
Neohelikian Coppermine River Group. Mineralization is exposed
intermittantly over 213x4.5 m. Resources calculated in 1969 are
listed as 1,000,000 tons at 2.5% copper.
The Muskox Intrusion is a layered ultramafic body containing
chromium, copper, nickle plus minor platinum and palladium.  The
showing is situated in the northwestern portion of the Bear
Structural Province and is of Mesoproterzoic age.  A 500 metre wide
feeder dyke to the intrusion is traceable for about 55 kilometres
south-southeasterly from the Coppermine River while a funnel-shaped,
layered complex is exposed for 50 kilometres north of the
Coppermine River.  The width of the complex varies but has a
maximium width of 9 kilometres.  Exploration has been targeted on
the central layered portion and the marginal sulphide zones in the
complex.  Sulphides along the margin are generally greater than 1
percent and form two thick (60 to 350 metre) gossanous bands.  At
the intrusive/country rock contact layers to pods of massive
pyrrhotite (minor pentlandite and chalcopyrite) occurs.   A
chromite seam (38 centimetres thick) is exposed at the center of
the intrusion and a resource figure is reported for this layer
(GNWT RWED, MOG Book (1997)).
Lead and zinc sulphides occur as pods, lenses and in fractures in
sheared skarn at the contact of Cretaceous quartz monzonite with
Cambrian sediments. The main B zone is a vein system with sheared
carbonate replaced by sulphides. A resource estimate of 1,635 T/VF
at 5.12% lead, 5.42% zinc and 0.71 oz/ton silver was based on
mapping, trenching and sampling of the B zone in 1974. Diamond
drilling was done in 1975.
Mineralization exists as veins of massive argentiferous galena and
sphalerite plus tetrahedrite, minor chalcopyrite in a shear zone
hosted by cherty dolostone of the Ordovician Whittaker Formation.
The showing is situated at a facies change between platformal
carbonates and basinal calcareous shales of the Selwyn Basin.
Twelve zones of mineralized veins and and a few stratiform deposits
giving a total strike lenght of 20 kilometres.    Work done on the
showing includes: 1928: discovery 1959-60: staking, mapping and
trenching 1966-69: stripping, geophysics, diamond drilling, two
adits were driven with crosscuts 1970-74: diamond drilling,
drifting, raises driven, soil geochemical sampling, metallurgical
testing,  1974-75: recalculation of reserves, surface and
underground diamond drilling and tunnelling 1981-82: preproduction
development, a 1,000 ton per day mill erected  A resource estimate
of 2,143,000 tons (proven, probable and possible) at 10.9% lead, 13.
5% zinc, 0.52% copper, 0.087% cadmium and5.58 oz/t silver was
listed in 1974. In 1982 a resource calculation for Zone 3 was given
as 1,629,000 tons proven and possible at 11.16% lead, 12.17% zinc,
0.44% copper and 5.4 oz/t silver.  In 1995 the in situ metal
inventory was reported to be 565 kt zinc, 502 kt lead and 780 t
silver.
The Coates Lake showing has Zambian-type stratiform mineralization
consisting of pyrite, chalcopyrite, bornite, digenite, chalcocite,
covellite, plus malachite and azurite which is disseminated within
beds of Hadrynian limestone and dolomite at the transition between
red beds and grey Coppercap Formation limestone of the Hadrynian
Coates Lake Group.  The area is known as the Redstone Copper Belt .
The cooper-bearing rocks have a maximum thickness of 110 metres
and a strike lenght of 30 kilometres.  Work was done on the showing
site from 1960 - 1989 (when it was reassessed). Work includes:
geochemical sampling, geological mapping, geophysics and diamond
drilling (including 24,000 feet in 1976-77 by Shell Canada
Resources). Tonnage and grade were calculated for the B-1 copper
bearing bed that dips 30 degrees W with a strike length of 20,000
feet and continues downdip 8,000 feet.  Diamond drill indicated
reserves  are listed as: 37,000,000 tons at 3.9% copper, 0.33 oz/t
silver, over a thickness of 3.3 feet OR 20,500,000 tons at 4.2% Cu,
0.27 oz/t silver (1977).
Mineralization includes pyrite, chalcopyrite, bornite, digenite,
chalcocite and covellite in a lensoid Zambian type copper deposit
in do;lomites of the Lower Coppercap Formation at the top of the
Hadrynian Coates Lake Group within the Keele River embayment. A
resource was estimated at 1,200,000 tonnes at 2.7% copper across 12.
5 m (1976) - this estimate is based on diamond rilling (? amount).
June creek north located 1 mile N, keele west and trudy creek 0.75
mile E.
Mineralization consists of sphalerite and galena disseminated in
Middle Devonian bitumen-bearing limestone, it also appears to lie
along fault zones as fractures and breccia fillings.  Work done on
the showing area includes: 1967-74: trenching, geological mapping,
geochemical sampling, IP and diamond drilling 1987: sampling.
Potential resources indicated are: 1,000,000 tons at 8-10% lead
zinc.
Mineralization consists of disseminated pyrite, pyrrhotite and
minor chalcopyrite along thin fractures in bedded limey quartzite
and shale close to a granitic intrusion.  Work on the showing
included prospecting and diamond drilling (786 feet in 5 holes). An
inferred resource was calculated at 25,000 tons at 0.5% copper.
Mineralization consists of scheelite and chalcopyrite in garnet-
diopside and massive pyrrhotite skarns in Cambro-Ordivician wavy-
banded limestone unit adjacent to a Cretaceous quartz monzonite
stock.  Work done on the showing includes: 1960-61: staking,
geological mapping, diamond drilling 1967: restaking, soil sampling,
mapping, magnetic survey 1973: geological mapping, trenching 1977:
geological mapping, soil sampling, EM and magnetic surveys and
diamond drilling. Diamond drill indicated resources from 1986 are
listed as 750,000 tonnes at 1.17% WO3, and an estimated 0.15%
copper.
The Howard Pass (XY) deposit is a Silurian aged stratibound
sedimentary hosted zinc-lead showing located in the Cordillera
Structural Province along the NWT-Yukon Border .  The showing is
hosted in a chert, limestone and mudstone (slate) unit termed the
Active Member which obtains a maximum width of 50 meters in the
center of the unit, thining towards the outer margins.   The unit
is situated in a paleo-basin  which allowed concentrations of
sphalerite, galena and pyrite to accumulate.  Pyrite is strongly
associated with the occurance of sphalerite and galena.  Other
minerals associated with the deposit include nickel, colbalt,
arsenopyrite, stibnite and selenium.  The Active Member is sub-
divided into an upper and lower sequence.  The upper portion of the
unit is dominated by  carbonaceous chert while the lower portion is
limestone and cherty limestone along with some carbonaceous
mudstones (CIMM, Special Volume 37; referenced as V3719).
Mineralization occurs throughout the Active Member with erratic
occurances and a decrease in lead and zinc values along the thinner
margins.   The footwall sediments consist mainly of carbonaceous
mudstone with a reported thickness of 50 metres  while the hanging
wall sediments are phosphatic carbonaceous chert.  Both of these
units are black in colour and are eith massive to more commonly
laminated.  Some sphalerite, galena and pyrite occur within these
units but of much lesser concentration then within the Active
Member.
Work preformed on the showing include exploration diamond drilling
soon after the discovery in 1968.  An all-weather road was
constucted in the early to mid 1970s.  More recently , early 1980s,
underground exploration was conducted in order to bulk sample and
test (metallugical) the depost.  The showing has a drill-indicated
reserve of 59,000,000 tonnes grading 5.4 percent zinc and 2.1
percent lead.
Work done on the showing include: 1962-68: exploration and sampling,
geochemistry, mapping and diamond drilling 1973: An adit was
opened, crosscuts driven and underground diamond drilling done as
well as metallurgical testing 1974-77: environmental and
feasibility studies were done 1979-80: diamond drilling,
underground bulk sampling and ecological studies  were done  The
Mactung showing consists of two zones, in 1983, resources were
calculated: Lower zone: 6.1 million metric tonnes minable
underground at 1.16% WO3; Upper zone: 17.2 million metric tonnes
minable by open pit at 0.78% WO3.
The Bear-Twit showing has been subjected to geochemical sampling
and diamond drilling. Resources are listed as 8-10 million tons at
up to 5.4% zinc, 2.6% lead and 0.5 oz/t silver. Diamond drilling in
1976 by Bethlehem Copper Corp indicated the deposit to be sub-
economic.
This showing is a carbonate hosted zinc-lead deposit in the
Grainstone and Basinal Formations of the Hadrynian Little Dal Group.
Mineralization consists of sphalerite, galena,  and minor pyrite
in breccias of Mississippi Valley Type tabular to pillarlike bodies
near stromatolite reefs. Work done on this showing includes
geochemical sampling, IP, geological mapping, geophysics,
lithogeochem and diamond drilling (at least 89,400 feet in 169
holes). Resources are estimated to be 50,000,000 tons at 4.7% zinc
and 0.3% lead . Typical individual diamond drill indicated bodies
where zinc is greater than lead include: 56,300 tons at 14.52% Zn-
Pb; 95,000 tons at 9.85% zn-Pb and 1,066,800 tons at 4.51% Zn-Pb.
Crest is an iron deposit hosted in the Rapitan Group of glacial-
marine sediments containing a 150 metre thick hydrothermally
deposited iron formation of Late Proterozoic age.  The Rapitan
Group strikes southeast for 640 kilometres and obtains a width of
40 kilometres and has a basal unconformity related to rifting in
the Late Proterozoic.  This group of glacial-marine sediments is
conformably overlain by Cambrian aged shales and carbonates.   The
Crest showing is located in the northern portion of the Rapitan
Group in the Snake River area and is the most iron-rich portion of
the Rapitan Group.  The iron formation consists of 10 iron-rich
layers (each about 24 metres thick)  characterized by hematite-
jasper pistolite, pod and wave rhythmites.  The laminae within the
rhythmites are of millimetre to centimetre thick.  Hematite is the
iron-ore mineral within the showing which has a resource of 5.6
billion tonnes grading about 47.2% iron.      The region contains
the third largest deposit of iron in North America with a total
resource estimate of greater than 18.6 billion tonnes.  Iron
concentration was first note around the turn of the century (1906)
during the Klondike gold rush by prospectors.  But it was not until
1961 that an iron-enriched strata was discovered in the Rapitan
Group of sediments.    During the 1960 s at least 3048 metres (25
diamond drill holes) of diamond drilling, channel sampling and bulk
sampling  were completed in the Snake River basin.