S3J01NW00ie 2.36M ALJO LAKE010

SACHIGO RIVER PROJECT

REPORT ON GEOPHYSICS

V; .

R. ValliantLong Lac Mineral ExplorationJuly/1980

Location and Access)ca^j

The Sachigo River property is 250 miles north of Red Lake in the Aljo Lake Area, District of Kenora. It consists of 36 mining claims numbered KRL 503358 to 503368 incl. and KRL 510205 to 530209 inc3 . These are centered at 54 030'40" 3atitude, 91 O24'30" longitude within N.T.S. sheet 53J 11.

Access is provided by bush plane to Dorothy Lake.

Introduction and Previous

The Sachigo property contains the Sachigo River Exploration Co. Au mine which, during 3938 to 1943 produced 52,560 02 Au and 6,127 oz. Ag from 46,416 tons of ore (Edwards, 1944). The property has been dormant since 1943 with limited surface exploration conducted by Great Plains Dev. Co. (1972) and Flint Rock Mines Limited (3961). Diamond dri33ing of geophysical anomalies and Au- bearing quartz veins was done by Great Plains Dev. Co. (1972), Flint Rock Mines Limited (1961) and Canadian Nickel Co. Ltd. (1974). Airborne magnetic surveys by the Geological Survey of Canada (1965, 1966) and an Input MK IV survey flown for Great Plains Dev. Co. (3972) provide regiona3 geophysical data. Results of these surveys are on file at the resident geologists office, Red Lake, Ontario.

Long I, ac Mineral Exploration Limited optioned the property in the spring of 1980 to re-evaluate its potential to contain economic gold mineralization. Magnetometer, V.L.F. and geological surveys were conducted over the mine area. The magnetometer survey was necessary because a previous survey (Flint Rock Mines Limited, 1961) did not correalate with geological data. V.L.F. surveying was conducted as a rapid means to detect disseminated sulphide mineralization.

Survey Methqdjs

Survey stations 100 feet apart were located on north trending, f3agged, pace and compass lines at 300 foot spacing. An east-west base line through the mine headfraree was used to tie the lines together. The lines are concident with a grid established by Huntex Limited during a biogeochemical sampling program (3978, 1979).

Magnetic susceptabi ] i ty of rock units was measured using a McPhar M-700 fluxgate magnetometer. A permanent base station was established at line 12 west, 100 north. The instrument was calibrated to 3,000 gammas and read twice daily at the base station to check for drift. Stations on the base line were used to close survey 3ines and measure diurnal variation. Diurnal variation and drift were negligable (- 20 gammes) during the survey period.

V.L.F. surveying was done using a Geonics E. M. - 16 receiver. Cutler, Maine was used as the transmitting station. Dip angle and out-of-phase readings were taken at the same location as the magnetometer survey. Frazer contour maps (Frazer, 1969) were used for final data interpretation.

. ..2

-2-

Values range from 2800 gammas to 7000 gammas and are disposed about broad south-east trending areas.

Government aeromognetic maps at l inch to l mine illustrate this southeast trends. Prenounced lows southeast and west of the survey area and an increase in total field magnetic intensity to the north are major regional

features.

Magnetic highs ()4800#) are: 1) a 1200 foot linear zone, azimuth 110 located 600 feet northeast of Grace Lake.

2) a 400 foot linear zone, azimuth 100 located 1300' south of l (above).

3) a single point high at the north end of

line 6 east.

4) two single point highs at the northeast side of Foster Lake.

5) a single point high on line 36 east 9 + 00

south.

Numbers l, 2 and the southern point of 4 correalate with magnetic anomalies discovered by Flint Rock Mines Limited (1961).

Magnetic lows (4.3800 gammas) are: 1) a discontinuous 1400' linear zone located 300 feet north of mag. high 1.

2) a broad southeast zone located between Foster and Dorothy Lakes.

3) two points at the south of lines 3 west and 6 east.

4) two parallel zones approx. 1200 feet long at the S. E. of the grid.

Intermediate magnetic values O4200 gainmas and ^800 gamines) are concentrated in the western part of the survey area. The eastern section has a relatively constant, low response averaging 4000 gainmas. A second area of uniform, low magnetic response is a 1200 foot wide, southeast trending zone at the south end of Foster Lake.

A quartz diorite to granodiorite stock crops out at the south of Foster Lake coincident with the low magnetic response.

In general these results correalate with these of the Flint Rock Mines Ltd. (1961) survey. The Flint Rock low between Foster and Dorothy Lakes is confined to a northeast zone joining the mine area. The location of most anomalous areas varies between the two surveys by up to 200 feet. This may be due to inaccurate location of survey stations or poor base maps.

.. .3

-3-

Kafic volcanic and intrusive rock underlying the survey area contain

l percent magnetite and do not have an appreciable magnetic susceptibility to permit accurate correalation of units.

Rejnjltsof V.L.F. Survey

The response of the V.L.F. unit within the survey area was, in general poor due to the wet muskeg cover. Plotting of out-of-phase profiles result in too many crossovers to properly interpret. Data was illustrated using the Frazer method (Frazer, 1969) which resulted in a more systematic distribution of anomalies.

The greater than 460 values can be divided into two groups which are at two distinct orientations. The first, at 100 to 110 is best represented by a strinq of anomalies from north of Grace Lake to the south end of Dorothy Lake (figure l, anomaly la-e). Canadian Nickel Co. Ltd., (1974) drilled two holes 300 and 500 feet north of anomaly IB. These holes intersected andesite and felsic tuffaceous rock with up to 13*1, pyrite plus pyrrhotite and traces of sphalerite and chalcopyrite over widths up to 4 feet. No assays are given. This drilling was done near a six channel Input anomaly and a Sharpe SE200 ground conductor (Flint Rock Mines, 1961) but did not intersect the E.M. 16 anomaly.

. Two anomalies of the east of Dorothy Lake form a zone, azimuth 100 (fig. l, anomaly 2) which has a strike length of 1800 feet. A Sharpe S.E. 200 anomalie (Flint Rock Mines, 1961) is approximately 300 feet south of this zone. These have not been drilled.

A number of isolated conductors, belonging to Group l include the following.

Anomaly 5 is a 900 foot long, east trending, linear zone at the south of Sherman Lake within the quartz diorite to granodiorite stock. Quartz-tourmaline pyrite veins are near its west extent. Diamond drilling of the original Foster Lake Au showing (Flint Rock Mines Ltd., 1961) was at the northeast flank of the zone however no conductive material was observed in core.

A strong, 1200 foot linear anomaly, azimuth 80 is at the base line between lines 15 west and 27 west. This, has been intersected by Flint Rock diamond drill holes S-ll and S-12. Quartz stringers with pyrite, in places assaying up to 0.10 oz Au per ton were intersected in hole S-ll.

A 900 foot, east trending zone northwest of Dorothy Lake (Fig 2, anomaly 7) correalites with a Sharpe S. E. 200 anomaly (Flint Rock Mines, 1961). No geological information is available to explain this anomaly.

Anomalies 8 and 9 form a broad, discontinueous, east-trending zone. No geological information is available to interpret these conductors.

The second group of anomalies, azimuth 60 is less distinct than the first. These occur 1200 feet east (fig. l anomaly 3) and 1200 feet west (ie. l, anomaly 4) of the center of Foster Lake. These may be related to faulting. Volcanic units east of Foster Lake are difficult to trace past the location of the V.L.F. conductor. The 60 trend may also be due to the method of data presentation. High areas correalate well with flanking east trending anomalies as with anomaly 3b and 5 (fig. 1).

...4

-4

ConclusLrs and Recommendaions

Relative magnetic susceptibility between rock units is low, therefore

magnetic contours cannot be used to trace the extent of rock units. Magnetic

anomalies may be usefu] as expressions of sulphide mineralization where coupled

with an E. M. conductor.

V.L.F. surveying outlined zones containing bedrock conductors, however

in general the machine responded poorly due to extensive conductive overburden.

Many of the isolated Frazer highs and broad high areas may be due to overburden

effects.

Conductors numbered l, 2 and 5 (fig. 1) may be due to Au-bearing sulphide

mineralization. These have not been observed on surface and have not been

intersected by diamond drilling. The surface expression of these conductors

should be accurately located by means of vertical loop crossovers or I. P.

surveying on a cut grid. Diamond drilling of conductors which respond

to I. P. is warranted.

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J

LEVITT LAKE AREA

53j0iNweeie e.36H ALJO LAKE 020

SACHIGO RIVER PROJECT

REPORT ON GEOLOGY

R. ValliantLong Lac Mineral ExplorationJuly, 1980

I XD caton and

The Sachigo River property is 250 miles north of Red Lake, Ontario in the Aljo Lake Area, District of Kenora. It consists of 16 mining claims numbered KRL 510205 to 510209 incl. (fig.l) These are centered at 54 030'40" latitude, 91 O24'30" longitude within N.T.S. sheet 53J 11.

Access is provided by bush plane to Dorothy Lake.

and Previous Work

The Sachigo property contains the Sachigo River Exploration Co. gold mine which, during 1938 to 1943 produced 52,560 02. Au and 6,127 oz. Ag from 46,416 tons of ore (Edwards, 1944). The property has been dormant since 1943 with limited surface exploration and diamond dril ling conducted by Flint Rock Mines Ltd. (1961), Great Plains Develop ment Co. Ltd. (1972) and Canadian Nickel Co. Ltd. (1974). Airborne mag netic surveys by the Geological Survey of Canada (1965, 1966) and an Input MK IV survey flown for Great Plains provides regional geophysical data. Results of these surveys are on file at the resident geologists office, Red Lake, Ontario.

Geological surveys of the Sachigo River area began with Meen (1937) who described the west part of the Blackbear River - Ellard Lake green stone belt. The area received little attention until Bennett and Riley (1969) published a short description of the area. Geology of the mine is described by P'dwards (1944) and the mine property was mapped at l inch to 200 feet by Flint Rock Mines Ltd. (1961) . Summary descrip tions and production figures of the Sachigo Mine from 1937 to 1943 are contained in O. D. M. annual reports.

Geology of the Mine Area

The Sachigo property is within the 55 mile long Blackbear River - Ellard Lake metavolcanic - metasedimentary belt. The belt contains an - estimated 80 percent mafic volcanic rock, 15 percent felsic volcanic rock and 5 percent sedimentary rock (Bennett and Riley, 1969).

Mafic rock consists of:

1. banded plagioclase (aligoclase to andesine), hornblende and epidote rich amphibolite

2. volcanic rock comprised of plagioclase (albite to Na - andesine), blue-green amphibole, biotite, clinozoisite and accessory quartz, carbonate, leucoxene, Fe - Ti oxides, pyrite and apatite.

Felsic rock predominates at Ellard Lake and between Chick and Guminer Lakes. Fragmental rock is more common than massive flows. Conglomerate lenses up to 1000 feet thick and intercalated greywacke is south of Sherman Lake and west of Ellard Lake. The 8 mile long Ellard Lake granite, to quartz monzonite stock intrudes the west end of the belt. Quartz diorite to granite dikes, sills and plugs are distributed throughout the area,

2.

The mine area is near the middle of the greenstone belt. It is

underlain by alternating basalt flows and gabbro sills which comprise a

total apparent thickness of 2.5 miles. Volcanic rock is thought to be

folded about an east syncline (Bennett, 1944) and intruded by a 2000

feet long by 800 feet wide quartz diorite to granodiorite plug at the

south of Foster Lake. Narrow quartz and feldspar porphyritic dykes

intrude the volcanic rocks. Felsic ash and quartz-feldspar cyrstal

tuffs are l percent of the rock as interflow pyroclastic material.

Stratigraphic facing directions are difficult to determine from

available exposure. Contact relationships between mafic flows and

felsic ash tuff, observed west of Foster Lake suggest south tops.

Volcanic units strike approximately 110O , dipping 70O south to vertical

throughout the map area. In places, a poorly developed cleavage is

parallel to volcanic units within basalt and tuffaceous rock.

Basalt is dark green weathering l m. to 15 m. thick, massive and

pillowed flows which have flow top breccias, pillow breccias and lenses

of hyaloclastic rock at interflow positions. The rock varies from a

very fine grained, 60 percent, felted amphibole matrix to l mm. sub

hedral plagioclase and 2 mm. amphibole phenocrysts in a fine grained

plagioclase, chlorite, amphibole matrix. In places, flows contain up

to 6*i carbonate amygdules, l percent pyrite and minor quartz crystals.

Three types of alteration are present. These are:

1. silicification along reguarly spaced fractures, flow contacts,

pillow boundaries or around fragments. Silicification is

intense 400 to 600 feet north east of the mine headframe.

Patches of silicified basalt are present within most lax'ge

flow units on the property.

2. Epidotization is, in places, quite common. This produces a

bleached white to light green weathered and fresh surface.

3. Chlorite overgrowing amphibole and filling fractures is common

in the basalt, however, not as intense as silicification or

epidotization.

Gabbro sills are massive with 1.5 mm., equigranular plagioclase,

and amphibole forming the bulk of the rock. Units are coarser grained

towards their center and in places, amphibole is up to 5 mm. in diameter,

The maximum dimension is 500 feet thick by 4400 feet long, however, the

sills average 80 feet thick by 1000 feet long.

West of Foster Lake gabbro dykes cut a coarser grained gabbro sill.

These dykes are identical in appearance to massive mafic flows, sug

gesting that they may represent feeders to overlying flows. This dates

the emplacement of sills as being very soon after deposition of over

lying volcanic rocks.

Felsic rock is predominately white to buff weathering, light grey-

green to brown, quartz and feldspar porphyritic dacite. Plagioclase

3.

crystals are subhedral, slightly resorbed, chlorite and sericite altered,

They may be up to 6 nun. long comprising 25 percent of the rock. Quartz

crystals are l to 2 mm. long, lense shaped and may comprise up to 10

percent of the rock. In places, l mm. amphibole phenocrysts are up to

15 percent. Pyrite is trace to 2 percent. Contacts are irregular,

branching of the dykes commonly occurs and fragments of adjacent rock

are within felsic material near the contacts. This indicates that the

majority of felsic rock underlying the property is intrusive.

Ash and lapilli crystal and lithic felsic pyroclastic rock is at

certain basalt flow contacts in the south half of the property. At

outcrop S 80-31 (fig. 2) the rock is 20 percent l to 4 mm. plagioclase

crystals, 4 percent l mm. quartz crystals, 12 percent wispy chlorite

or amphibole fragments (pumice?) and l percent basalt fragments up to

10 cm. in diameter. Crystal tuff is similar to felsic intrusive rock

except that grain size sorting and concentration of crystals into bands

produces a distinguishable bedding. Pyrite averages l percent, however,

may be up to 10 percent over 10 cm. thick, lensy beds. In places,

pyrrhotite predominates over pyrite, however, no pyrite - pyrrhotite

zoning was recognized.

A zoned quartz monzonite to quartz diorite stock with an outcrop

area of 1800 feet by 800 feet intrudes volcanic rock south of Foster

Lake. Quartz monzonite is west and south of quartz diorite. In

general, the rock weathers light grey and consists of l to 2 mm.

equigranular quartz (10%) , biotite (up to 124) , amphibole or chlorite

(10**,) , plagioclase ( 45*) , pink K-spar (15%) , pyrite 14 and variable

amounts of epidote and sericite. Quartz diorite has greater biotite

and amphibole and no K-spar. At the south east of Foster Lake quartz

diorite is intruded by l cm. to l m. thick dykes of quartz monzonite.

In places, this produces a diorite fragment breccia. Randomly oriented

quartz veins up to 45 cm. thick are less than l percent of the quartz

diorite.

Economie ^

The number l Sachigo Au showing is a quartz vein striking 030O ,

dipping vertical within the quartz diorite. This vein was traced for

450 feet and is reported to contain 0,30 oz. Au per ton over 2.5 feet

(O. D. M. report, Mineral Deposits file). Nine diamond drill holes by

Flint Rock Mines Ltd. (1961) did not reproduce these results. The

vein could not be located at surface for sampling during the present

survey. Two veins south of Foster Lake containing up to 20 percent

tourmaline and minor pyrite were sampled for Au assay. The diorite

bounding the veins is bleached and sericite rich over 5 cm.

The Sachigo River gold mine, north of Foster Lake was mined at

8 levels from a 2 compartment vertical shaft 1,139 feet deep (O,D.M, f

1942). The ore zone occured between a massive coarse grained footwall

flow and a fine grained hanging wall flow. The zone consisted of

erratic quartz veins separated by schist or brown fe-Jdspar porphyritic

dacite with blue quartz eyes (Edwards, 1944). Three types of quartz

were described by Edwards. These are:

4.

1. dark blue-grey, narrow lenses containing pyrite, sphalerite,

pyrrhotite and galena. Gold averaged 4 ounces per ton and

silver was up to 25 oz. per ton.

2. grey-white quartz lenses averaging 7 feet wide with 150

foot vertical extent. The veins contain pyrite, chalcopyrite,

pyrrhotite, sphalerite and galena. Fine disseminated Au was

near vein contacts giving an average grade of 0.5 to 1.0 oz.

per ton.

3. clear, friable glassy quartz containing very low Au associated

with pyrite. Coarse Au flakes may occur near dacite contacts

and minor chalcopyrite and galena are reported.

Similar contact relationships between volcanic units were noted at

a number of localities within the map area. Stratiform zones of quartz

veining were not observed at the coarse grained - fine grained and dacite

contacts. Isolated, randomly oriented white and grey-white quartz veins

with tourmaline, carbonate and pyrite cut all rock types on the property.

The thickest and most extensive of these were sampled for Au assay (ap

pendix 1). Limits of diamond drilling along strike from the ore zone

are not known. Flint Rock Mines (1961) drilled 3 holes west of the mine

workings. Biotite diorite, basalt and syenite porphyry were intersected.

Quartz stringers assaying up to 0.16 oz. Au per ton over 1.5 feet,

however, most assays returned only trace Au. If the ore zone is pro

jected westward at 105O , the average strike of volcanic units, these

drill holes do not extend far enough north to intersect it.

Tuffaceous interflow sediments up to 15 cm. thick containing up to

lOt pyrrhotite, 2 !fe pyrite and traces chalcopyrite were observed at a

number of localities within the property (figure 2). These are pre

dominately fine grained, chlorite and carbonate bearing ash tuff as

discontinuous lenses overlying basalt. These were sampled for Au assay -

{appendix 1).

Flint Rock Mines Ltd. (1961) drilled l diamond drill holes, at the

south half of Dorothy Lake to test geophysical conductors. Holes 4, 5

and 6 are at azimuth 320O and may have tested the possibility of Au-

bearing fault zones along an assumed northeast structure through Foster

and Dorothy Lakes. These holes intersected basalt and quartz prophyry.

No significant sulphide or Au mineralization is reported.

Sludge samples from hole number l contained 0.01 oz. Au per ton

over 0.5 feet, 0.11 oz. Au per ton over 5 feet and 0.02 oz. Au per ton

over 3 feet. Sludge from hole 2 is reported to contain O.OG oz. Au per

ton over 1.5 feet.

Also of interest are 2 diamond drill holes northwest (Canadian Nickel

Co. Ltd., 1974) and 2 holes east-northeast (Great Plains Dev. Co. Ltd.,

1972) of the map area. These are drilled within a broad zone of input

and V.L.F. conductors, azimuth

5.

The Canadian Nickel ho]cs intersected up to 15 percent pyrrhotite, l percent pyrite with traces of chalcopyrite and sphalerite over a zone

40 feet wide, however, no assay values are given. The sulphides are within felsic tuffaceous rocks intercalated within andesite and dacite flows. The holes drilled by Great Plains Development Co. Ltd. intersected a variety of felsic rock with graphitic zones containing up to 20 per

cent pyrrhotite. No assays are reported for these holes.

During the present survey, samples were collected from the remains of an ore dump, waste and rock dumps and selected outcrops. Results of Au assays are pending. Two samples of quartz vein material from rock dumps near the headframe were analyzed for Au content by the O.G.S. (1980).

These have values of 4.58 oz. Au, 0.42 oz. Ag per ton and 2.12 oz. Au, 0.64 oz. Ag. per ton (M. Durocher, pers. comm., 1980).

Conclusions

Gold occurs in two environments at the Sachigo property. These are:

1. gold bearing quartz veins within the quartz diorite phase of the Foster Lake stock and

2. gold bearing quartz veins, lenses and adjacent schistose rock at the contact between mafic lava flows.

Examination of rock at the Sachigo mine site indicates that type 2 mineralization is, in part, sedimentary and accumulated during a hiatus

in volcanism. The schistose rock is a mixture of tuffaceous material and chemically precipitated clay minerals. Au-bearing, conformable quartz lenses are recrystalli zed chert beds. The dacite may be either felsic crystall tuff or intrusive rock.

Thin beds of pyritic tuff were located during geological mapping. If these contain gold they should be traced by detailed geophysical sur veys. No specific drill targets can be recommended until geochemical analysis of samples is completed.

The predominance of mafic volcanic and intrusive rock underlying the map area and drill intersections of felsic rock to the north indicate that gold mineralization is within the mafic part of a bimodal volcanic

sequence. The numerous mafic and felsic dykes and their relationship with a quartz monzonite - quartz diorite stock suggests that rock underlying the property is within the "root" zone of an Archean volcanic center. Sulphide bearing felsic rock northwest and east of Dorothy Lake may represent top of cycle, volcanic material and deserve more detailed exploration.

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22

LEVITT LAKE AREA

Ontario

Ministry of Nati

GEOPHYSICAL - GEOLOG TECHNICAL DAT

53J01NWOG)ie 2.36M ALJO LAKE

TO BE ATTACHED AS AN APPENDIX TO TECHNICAL REPORTFACTS SHOWN HERE NEED NOT BE REPEATED IN REPORT f.A

TECHNICAL REPORT MUST CONTAIN INTERPRETATION, CONCLUSIONS ETC.

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GEOPHYSICAL - GEOLOGICAL - GEOCHEMICAL TECHNICAL DATA STATEMENT

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