ne r 22 1 0q7 - ontario

31C11SWW16 2.1*671 MADOC 010

REPORT ON

THE MOIRA LAKE TALC PROSPECT

MADOC TOWNSHIP. ONTARIO

N.T.S. 31C/11

Toronto, Ontario July 15, 1987

Ref.: 87-57

PREPARED FOR

MARADONA RESOURCES INC.

DERRY, MICHENER, BOOTH 6c WAHL

P. A. Hartwlck, B.Sc.RECEIVED

ne r 22 1 0Q7

MW4WG IAHOS SECTION

This report may not be reproduced, in whole or in part, without the written permission of Derry, Michener, Booth fa Wahl.

DEKRY. MICHENER. BOOTH ft WAHL

TABLE OF31CHSWM16 2.1*671 MADOC O10C

J

SUMMARY

INTRODUCTION

PROPERTY LOCATION, DESCRIPTION AND ACCESS

TOPOGRAPHY AND VEGETATION

ECONOMICS OF TALC

REGIONAL EXPLORATION HISTORY

PROPERTY EXPLORATION HISTORY

REGIONAL GEOLOGY

REGIONAL TALC MINERALIZATION

CURRENT PROGRAM

PROPERTY GEOLOGY

Stratigraphy Structural Geology

THIN SECTION ANALYSIS

DISCUSSION

CONCLUSIONS AND RECOMMENDATIONS

PROPOSED PROGRAM AND BUDGET

REFERENCES

CERTIFICATES OF QUALIFICATION

J.J. Mayer, B.Sc. P.A. Hartwick, B.Sc.

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Colour cUpUeoAes to ere fiUcicA -from

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TABLE OF CONTENTS (Continued)

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LIST OF APPENDICES

APPENDIX It APPENDIX II:

APPENDIX III: APPENDIX IV:

Rock DescriptionsPhotographs of Trenches, Rock Types

and StructureThin Section Analysis and Summary Diamond Drill Log, Hole MDR-87-1

Figure 1: Figure 2: Figure 3: Figure 4:

Figure 5:

Figure 6:

LIST OF FIGURES

Location MapClaim MapRegional Geology, Madoc AreaSimplified Geology of the

Moira Lake Property Detailed Geology and

Sampling of Trench 325E Section 05+OOE

After Page

l l 5

89

LIST OF MAPS (In Map Pocket)

Map 87-57-01 Property Geology, Moira Lake Property

DERRY, MICHENER. BOOTH ft WAHL

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SUMMARY

The Moira Lake property consists of four contiguous unpatented mining claims covering about 95 hectares, held by Maradona Resources Inc. The claim group is located in Madoc Township, Ontario, about 180 km northeast of Toronto

and 40 km north of Belleville. Access to the property can be made by road, about 800 m south of Highway #7 and 4 km east of the village of Madoc. The property is about 2 km northeast of the currently producing Canada Talc Industries Ltd. (Cantal) Mine.

Mapping, trenching and a diamond drill hole revealed that the Moira Lake

Property is underlain by the same stratigraphic and intrusive units found at the Cantal Mine site. A magnetic and VLF electromagnetic survey conducted on the property by Hansen (1985) located a conductive horizon about 75 m to 100 m north of the granite contact which was found to be a metapelite unit. The composition

and position of the metapelite unit is similar to that of the metapelite unit found on the footwall side of the talc deposits at the Cantal Mine. Intense microfolding

and moderate shearing found within this metapelite horizon and in units in

immediate contact with it, suggest that the metapelite is faulted parallel to the granite contact. This faulting may have provided a conduit for talc-forming hydrothermal fluids to reach the dolomitic marbles in contact with the

metapelite, north of the granite body.

DERRY. MICHENER. BOOTH ft WAHL

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INTRODUCTION

This report, prepared by Derry, Michener, Booth It Wahl (DMBW) on

behalf of Maradona Resources Inc. (Maradona), summarizes the results of the Phase I exploration program carried out on the Moira Lake Talc prospect, located

near Madoc, Ontario. The program was carried out from April 29 to May 31, 1987 and consisted of linecutting and chaining, geological mapping, trenching, sampling

and diamond drilling. The geological mapping, core logging and field supervision was carried out by J. J. Mayer, B.Sc. and the program was carried out under the supervision of P. A. Hartwick, B.Sc.

The Moira Lake property is located about 2 km northeast of the currently producing Canada Talc Industries Ltd. (Cantal) Mine which, up to the end of 1984,

had produced approximately 890,600 tons of ore, a large proportion of which was of very high grade.

The property is underlain by the same stratigraphic and intrusive succession that exists at the mine and may have been subjected to similar metamorphic processes that were instrumental in the formation of talc.

PROPERTY LOCATION. DESCRIPTION AND ACCESS

The Moira Lake property is located in Concession IX, Lot l, of Madoc Township, Ontario, about 800 m south of Highway 7 and 4 km east of the village of Madox, as shown in Figures l and 2. The property consists of four contiguous unpatented mining claims, E0921259, EO921260, E0921261 and E0921262 covering

approximately 59 hectares.

Access to the property can be made by driving east on Highway 7 from

Madoc for a distance of about 4 km, then south on the all-weather gravel Pinewood Lake Road for a distance of about 800 m. The road is in proximity to the western boundary of the claim group. An abandoned northeast-trending

railway line provides excellent automobile access to the centre of the property.

DERRY. MICHENER, BOOTH ft WAHL

MOIRA .AKE PROPERTY

3^U.S. A.

toronto

Peterborough

Oshawa

oIE

tori 0

Seal* l: BOO 000

16 32kmZJ

MOIRA . LAKE X PROPERTY

Madoc

Belleville

Figure l

LOCATION MAP

CANADATALC INC.

MINE

Huntingdon Twp. l Hungerford Twp.

Scale l inch to 1/2 mile

O 1/2Figure 2

CLAIM MAP

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TOPOGRAPHY AND VEGETATION

The property has a maximum relief of about 25 m. The highest point,

about 185 m above sea level, is on the township line at the south edge of the

property and the lowest point, about 160 m above sea level, is a swampy area near the centre of the property.

Vegetation consists of poplars and cedars interspersed with grass and

scrub-covered fields in the northwest portion of the property, alders and

bullrushes on the low-lying, swampy ground in the centre, and mixed coniferous

and deciduous trees on the higher ground to the south. Areas of very thick poison

ivy growth were encountered in the central portion of the property where sand

and gravel overburden is abundant.

ECONOMICS OF TALC

Talc is predominantly used as a filler and whitener in products such as

pulp and paper, paints and varnishes, plastics, rubber and roofing products. During

the last few years, talc production in Canada has been about 95,000 tonnes per

year; 40,000 tonnes of which are consumed domestically and 55,000 tonnes of

which are exported, mostly to the U.S.A. (Industrial Minerals, January 1986).

Prices for talc range from about U.S.|40 for dark, impure talc, to over U.S.SSOO

for white, fine grind, essentially pure talc. The Henderson orebody at the Cantal

Mine contains very pure, white talc which sells for up to U.S^ISO per tonne

(99.996 minus 44 micron) and is used chiefly by the plastics and pulp and paper

industries. The company is currently expanding its processing facilities to

produce fine grind 10 and 20 micron products which can be sold for significantly

higher prices.

The United States is by far the leading consumer of talc in the world and,

therefore, represents an excellent potential market for Canadian producers. The

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OMadoc area is well situated to take advantage of a large market in the northeastern U.S.A. and eastern Canada. The discovery of a high grade talc deposit similar to that which exists at the Cantal Mine would be commercially

viable, assuming efficient mining and milling methods are maintained and the products are aggressively marketed.

REGIONAL EXPLORATION HISTORY

Madoc has been a centre of mining in eastern Ontario for well over 100 years (Hewitt, 1968). In 1837 Uriah Seymour built a furnace for smelting iron ore

and opened the Seymour iron mine, which operated from 1837 to 1845. Both hematite and magnetite were extracted from various mines in the region up to 1910.

In 1866, the first gold discovery in Ontario was made at the Richardson Mine near Eldorado. Two gold mines operated in the Eldorado area during the

period from 1894 and 1901. Lead, copper and pyrite were also produced from small mines in the early 1900s.

\The area is best known, however, for the production of industrial minerals

and building products. In addition to talc, which is and has been by far the most valuable commodity, fluorspar, marble, slate, granite, sand and gravel have been produced intermittently since the year 1900.

The first discovery of high grade talc mineralization in the Madoc area was made in the 1880s near the current Cantal mine site by Alexander Henderson while he was ploughing his field (Simandl and Ogden, 1982). Mining of the Henderson orebody began in 1896 and open pit mining was carried out until 1908 at which point underground operations began.

In 1911, the Conley orebody was discovered immediately along strike to the northeast of the Henderson mine and production on that property began in 1912. The two mines were merged into the Canada Talc Company (later to


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become Canada Talc Inc.) in 1929. Talc production has been almost continuous

from initial production in 1896 to the present, making the mine the oldest, continuously producing talc mine in North America. Total talc production from the Madoc deposits up to the end of 1984 was approximately 890,600 tons (Hewitt, 1972 and Roberts, 1985).

In addition to the several shafts that have exploited the Cantal deposits over the years, five shallow shafts were sunk to the northeast of the mine area to explore talc-rich zones, as shown in Figure 3.

In 1917 and 1919, International Pulp Company sunk three shafts within 800 m northeast of the Cantal East Zone. The shafts are 8 m to 18 m deep with a total of 75 m of drifting. Rock dumps near the shafts consist of grey to white massive talc and talc schist, talc- tremolite schist, dolomitic marble, and mica schist.

In 1941 and 1942, the Trent Mining Syndicate Ltd. sunk two shafts on the Price mine, located less than 100 m northeast of the East Zone on the Cantal

property. The principal shaft is 27.5 m deep with levels at 12 m and 24 m. Hewitt (1972) reported that the talc occurs in a narrow (0.6 m to 1.5 m) sericite- talc schist zone and strikes at 010 O, dips at 55O west, and is exposed for about 43 m along the 12 m drift. The zone strikes approximately parallel to the dolomite wall rock.

During the summer of 1981, Canada Talc Ltd. carried out a program of

surface mapping and diamond drilling which served to outline a new talc deposit called the East Zone, located about 100 m east of the Henderson deposit (Simandl and Ogden, 1982). Currently, the zone produces an average of about 25,000

tonnes per year to supplement the lower grade talc market (Roberts, pers. comm., 1986).

DERRY, MICHENER, BOOTH flt WAHL

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PROPERTY EXPLORATION HISTORY

The Ontario Geological Survey Assessment Files have records of two

exploration surveys having been carried out on the property. In February 1984, G. Pearse performed a magnetic survey to aid in mapping the assumed favourable

contact between the granitic intrusive and the dolomitic marble. The survey was apparently performed with insufficient diurnal control and consequently the survey has little technical value.

In February 1985, Trisar Resources Ltd. performed linecutting and a magnetic and VLF-EM survey on 100 m spaced lines with 25 m stations (Hansen, 1985). A discussion of the results and interpretation of this survey are given in

the Geophysics section.

Two diamond drill holes totalling 62 m were drilled on claim EO30565 (see Figure 2) located about 300 m to the north of the Moira Lake property. These

holes encountered dominantly white siliceous dolomite.

Records indicate that the Moira Lake property has undergone very little exploration work although the ground was held under lease for much of this

century and therefore work may have been performed but was not recorded. Discussions with mining engineers at Cantal and local individuals, however,

support the notion that the property has undergone only limited work.

REGIONAL GEOLOGY

The detailed geology of the Madoc area is described by Hewitt (1968) and is shown in Figure 3.

The Madoc area straddles the Paleozoic-Precambrian unconformity. Medium- to high grade metamorphic rocks of the Grenville Province lie to the

north and younger essentially unmetamorphosed sedimentary rocks of Ordovician- J age lie to the south. Flat-lying outliers of Ordovician limestone locally rest upon

DERRY. MJCHENER. BOOTH ft WAHL

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LEGEND

PLEISTOCENETill, sand, gravel, clay, marl.

11 Black River limestone. 11a Basal conglomerate.

UNCONFORMITY

PALEOZOICORDOVICIAN

not mapped

MOIRA LAKEv ,- PROPERTY* \ *C ;

H(JNTINGDONf TWP HUNGERFOROTWR

Figure 3REGIONAL GEOLOGY

- MADOC AREA -

(from OOM Map 2154 )

Scale: 1 inch to 1/2 mile

Granite and syenite undifferenti-

7 Dtoritrtnd gabbro undifferentlated. 7a Gabbro.

INTRUSIVE CONTACT

METASEDIMENTS AND METAVOLCANICS

SEDIMENTSQuartzite ami qutrUo-feUspathkrocks.j*— j— it- reisnv,

5 Pelitic rocks.Sa56 Paragneifs.Se Schist.5d Conglomerate.

4 Marble undtfferentlated.4a Dolomitic marble.46 Calcitic marble.4c Ume silicate rock.4d Limestone conglomerate.

3 Partumphtbolite. 3a Garnet amphibolite.

METAVOLCANICS Basic Metavolcanics 2 Undifferentiated. la Amphibolite, amphibolite schist. Ib Massive andesite. 2c Agglomerate. 2d Tuff. !e Pillow lava.

Acid Metavolcanics 1 Rhyolite, la Rhyolite tuff. 1b felsite. 1c felsite breccia. Id Rhyolite breccia.

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the Grenville rocks north of the unconformity. A small outcrop of the Ordovician

sediments was mapped on the Moira Lake property (see Figure 4) and a l to 2 m thick outcrop (not shown on Figure 3) has been exposed at the east end of the East Zone open pit on the Cantal property.

The oldest rocks in the area are the Tudor volcanics, a series of dark green, mafic lavas that exist to the north and northwest of the Moira Lake property. The volcanism apparently ended with rhyolitic flows and tuffs which overlie the mafic volcanic rocks. Overlying the volcanics in a generalized and approximate order of deposition are chemical sedimentary rocks consisting chiefly of dolomitic and calcitic marbles, which host the Cantal talc deposits and underlie

the Moira Lake property; fine to coarse-grained pelitic rocks most of which are now strongly schistose; and minor quartzite and quartzo-feldspathic rocks. Hewitt (1968) noted that in many locations, the sediments are interfingered with the volcanics, indicating a gradual transition from volcanics to sediments.

Intruding the Grenville volcanics and sediments in the Madoc Township area are four main bodies of pink granite and syenite, the Moira Granite being the only one which occurs in the property area. The granite is about 4 km long by 2 km wide and outcrops in the northeast portion of Moira Lake, including the south portion of the Maradona property. The intrusive is a pink albite granite

composed largely of albite and quartz with minor microcline (Hewitt, 1968).

Thin east-west trending undifferentiated diorite and gabbro bodies outcrop immediately to the east and northeast of the property but, in general,

mafic intrusives are not abundant in the Madoc Township area.

REGIONAL TALC MINERALIZATION

Talc deposits in the eastern Ontario region are associated with two host

lithologies; carbonate metasediments and/or mafic intrusive/volcanic rocks. In both cases talc-bearing zones occur adjacent to later felsic intrusive bodies. Talc

in a mafic host usually grinds to a pale grey colour, whereas the carbonate-hosted


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talc, such as that present at the Cantal Mine, is usually very white unless contaminated by mafic minerals.

The Cantal talc deposits occur within a thick sequence of Grenville crystalline dolomites which contain various interbeds of metamorphosed

carbonaceous and pelitic units. The orebodies strike northeast and dip steeply to

the northwest, approximately parallel to regional stratigraphy, and are within 300 m of the Moira Granite contact. Detailed structure of the deposit area is not well understood because of the general lack of outcrop and because the old mine

workings were not mapped. Hewitt (1972) concluded that the talc deposits occur on the south limb of an anticline that plunges to the southwest and that there is strong drag folding and crenulation on both arms of the fold. It would appear that

the bulk of the deformation occurred after the talc mineralization event(s) and that the deformation only served to alter the original shape of the zones.

The richest and best known of the orebodies is the Henderson deposit. It

consists of a steeply dipping, tabular sheet of pure white foliated talc with some local impurities of calcite, dolomite, pyrite and tremolite. The deposit is over

250 m long, 7 to 25 m wide, and at least 250 m deep, but is open at depth. The

footwall consists of dark grey to black phyllite overlain by irregularly banded micaceous dolomite containing coarse prismatic tremolite. The hanging wall consists of regularly banded micaceous and tremolitic dolomite containing some

grey siliceous bands. Next to this banded unit is a discontinuous tourmaline-

bearing layer overlain by quartz-bearing beds displaying stromatolitic texture,

"mottled blue" dolomite, and a thick dolomitic sequence containing local pyrite and amphibolite layers (Samandl and Ogden, 1982).

Based on general research by Hewitt (1972), the Madoc area talc

occurrences are hydrothermal replacement deposits. He postulates that

conformable sheet-like bodies of talc were developed from the Grenville dolomite by the introduction of hydrothermal solutions that probably originated from the neighbouring Moira Granite. Hartwick and Woolham (1986) summarized the

probable talc forming reactions and possible pressure-temperature-fluid

) composition constraints. The reader is referred to that report for a more complete discussion.


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North Baseline Grid Area

East Baseline Grid Area

T ^.^^-l.—.-——^

South Baseline \Grid Area

100 2 OO metres

9

5

LEG END

ORDOVICIAN

Basal Conglomerate

PRECAMBRIAN

Moira Lake Granite

Pelitic Sediments

Calcitic and Dolomitic Marbles

Lime-Silicate Rock

FIGURE 4

SIMPLIFIED GEOLOGY

OF THE

MOIRA LAKE PROPERTY

Scale K 5000

Dork shaded lenses contain small angular quartz fragments.

39

42

45

— 4bp

Unit contains very rare 1-2 mm and rhodochrosite stringers.

Zone with Imm to 10cm wide calcite stringers parallel to bedding.

4bp unit with Interbedded 4b-Intense microfoldlng visible throughout.-rare small quartz fragments.

O TS03

LEGEND

Microfolding with Plunge

Bedding

Channel Sample Location

Fine grained felsic intrusive

234 5 metres

FIGURE 5

DETAILED GEOLOGY AND

SAMPLING OF

TRENCH 325E

MAPN0 : 87-57-02

DERRY, MICHENER, BOOTH 8 WAHL

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CURRENT PROGRAM

The Phase I exploration program was carried out essentially as proposed by DMBW in Hartwick and Woolham (1986) although some minor changes were made as work progressed because outcrop exposure was better than expected in key areas of the property.

The surface work was controlled by three grids, separated by inaccessible swampy areas (Figure 4). A north base line was run from the northwest corner of the claims to the east to cover the north half of the property; a south base line was run from the middle claim post along the southern boundary to cover the southern portion of the property; and a southeastern base line was established to cover the southeastern part of the property. All base lines trend east-west at 070O and follow the claim line boundaries. For the north and south base lines, section lines were spaced 25 m and for the southeastern base line section lines were spaced every 50 m. All section lines were run perpendicular to the base lines at 160 O. The close 25 m spacing of section lines on the northern and southern grids allowed for detailed mapping and sampling where outcrop exposures were good and a detailed examination was deemed necessary. The large 50 m spacing of section lines on the southeastern portion of the property was sufficient due to the very poor outcrop exposure in the area.

Small and large scale trenching and stripping was performed using a D-6 bulldozer and a high pressure Wajax water pump. One large 500 m long trench (Trench 325E) (Figure 5; Appendix III, Plate 1) was cleared with the bulldozer and pump to expose a wide cross sectional area within the marble and several smaller areas were stripped using the Wajax pump where overburden cover was thin. Eighty-six grab samples were taken from the property, 22 of which were taken from Trench 325E. Of the surface samples taken, 31 were selected for thin section analysis.

Following the mapping, sampling and trenching, a 233.2 m (765 ft.) BQ-sized diamond drill hole, MDR-87-1, was drilled from near the centre of the

J claims towards the south to intersect the rock units which underlie the large


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swamp in the centre of the property (Figure 5 and 6). Sixteen samples were taken from the drill core, 9 of which were selected for thin section analysis.

A total of forty rock samples taken during the program were selected for thin section analysis. The purpose of the study was to detect microscopic minerals not readily identifiable in hand sample and to comment on mineral textures and phase relationships present, thereby intimate the general temperature-pressure regime which prevailed during the hydrothermal event(s).

PROPERTY GEOLOGY

Stratigraphy

The geology of the Moira Lake Property consists of a thick sequence of marbles and pelitic metasediments intruded in the south by a large granitic batholith, as shown in Figure 4. Bedding and contacts of all units strike roughly east-northeast and dip moderately to steeply towards the north.

Along the western boundary of the property and gradually thinning towards the east, exists a very thick sequence of calcitic and dolomitic marbles with minor interbedded pelitic material. Although the marbles tend to be massive (see Appendix II, Plate 2) and bedding cannot be recognized due to metamorphic recrystallization, where pelitic material is interbedded the orientation of the bedding is fairly consistent, trending between 060O and 080 O and dipping towards the north between 64O and 85O. In general, the amount of pelitic material interbedded within the marble increases towards the southern granite contact suggesting that there was a gradual progression from a carbonate to a detrital sediment-type environment.

Although the pelitic interbeds within the marbles can be very thick, as revealed in Trench 325E (Figure 5; Appendix II, Plate 3), along strike a single unit is very difficult to trace due to the interfingering nature of the "clean" marbles

) w ith the pelitic material, as illustrated in Plate 4 (Appendix H).


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CVIo

V)

8ro O

tn o m*8

MDR-87-1

en8•fS

X Ovirburatn

4b min p

LEGEND

~—~ Sheoring

*— Bedding

Vv Sample Location

See legend on Map 87-57-01

50 met res

FIGURE 6

SECTION 05400E02 + OOS to 04 + 50S

SCALE l! 1000

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OAlong the western boundary of the property the marbles are intruded by

numerous l cm to 30 cm wide discontinuous quartz veins, stringers and blobs. The presence of this quartz activity is encouraging as silica is a necessary component in the formation of talc and tremolite. Two occurrences of tremolite were found within the dolomitic marbles; one at N.L. 0+OOE 3+1 OS; and the other at N.L. 5+OOE, 2+OOS. Although tremolite is a detriment in talc ore, it is usually present in the wall rock of talc deposits because it is an essential constituent in the talc- forming reactions. The presence of tremolite on the property is therefore encouraging.

The number of pelitic interbeds and the ratio of pelitic sediment to carbonate sediment within a pelitic bed (i.e. clastic to carbonate ratio) increases towards the south contact with the Moira Lake Granite. Along the old railway bed, near the western boundary of the claims, numerous thin pelitic beds exist within the marbles which have been classified as true pelitic metasediments. This classification has been made based on the formation of large bladed kyanite crystals and the development of fine-grained muscovite flakes along bedding planes. Both these materials are metamorphic products of an aluminum and silica rich host.

\The southern limit of the true marbles is believed to be located near the

north shore of the large swamp. This is confirmed in diamond drill hole MDR-87- 01. This hole, drilled from N.L. 5+OOE, 2+158 towards the granite contact, intersected 47.87 m of "clean" dolomitic marble before entering a very thick sequence of pelitic metasediments. Some thin interbeds of dolomitic and calcitic marble are present within the pelitic sediments, as revealed along the southern shore of the swamp between S.L. 4+75W and S.L. 5+25W; however, these units tend to be very thin and discontinuous along strike.

The thick marble sequence gradually thins to the east and continues underneath the swamp off the Moira Lake claim group. This is confirmed in regional mapping by Hewitt (1968) as he found similar units farther to the east.


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The northeast portion of the property is underlain by a well bedded sequence of lime-silicate rocks striking roughly 060O to 080O and dipping towards the northwest between 650 and 80O (see Appendix II, Plate 5). Although these metasediments are carbonate dominated, they are not classified as true marbles or pelitic marbles because they have distinctly different characteristics. Generally, these sediments are more fine-grained with only patchy recrystallization to marble. The tan to pinkish-brown colour throughout this sequence is caused by a fine-grained arkosic constituent that is incorporated with the carbonate material.

The lime-silicate rocks interfinger with thin discontinuous beds and bands (less than l m wide) of detrital sediment in a similar fashion to that observed in the marbles towards the east and south. In this case, however, the sediment bands are of an arkosic rather than pelitic composition.

Locally, the lime-silicate rocks are intruded by small l cm to 5 cm wide discontinuous quartz veins and stringers. This quartz activity would ordinarily be encouraging for the formation of talc, but since none of the lime-silicate materialwas found to be dolomitic, no tremolite or talc formation was expected or found.

\The true pelitic metasediments occur wedged between the southern limit

of the marbles and the contact with the Moira Lake Granite as illustrated in Figure 4. These sediments range from thinly bedded carbonaceous pelites near the marble contact to more pure pelites in contact with the Moira Lake granite. Generally, the pelitic units are strongly bedded striking between 060O and 100O and dip steeply towards the north between 72O and 80O.

The northern contact of the pelitic unit is composed of a strongly bedded calcitic and dolomitic metapelite. This transitional unit represents a change from a carbonate to a detrital depositional environment. The contact between the true marbles and the pelitic units was found to be abrupt and was noted in outcrop at N.L. 0+25E, 4+30S and in drill core from hole MDR-87-1.

) Towards the granite contact, the detrital component of the pelitic unit increases with only rare, interbedded thin carbonate material noted. It is in this


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area that the argillite, phyllite and biotite-rich paragneiss are found. In general, the metamorphic grade and shear intensity, within the pelite, gradually increases towards the granite contact, reflected in the transition from argillite to phyllite up to the paragneiss at the contact. The argillite and phyllite are found to be continuous across the southern edge of this east-west trending swamp as illustrated on Map 87-57-01 (in map pocket). The biotite-rich paragneiss is not as extensive and is only found to exist between S.L. 3+75W and S.L. 5+25W, just south of the swamp.

The south-central portion of the property is underlain by a thick unit of very fine-grained, massive pelitic metasediment {see Figure 4) that was originally mapped as granite by Hewitt (1968) in Figure 3. In this unit faint bedding can only be recognized on the weathered surface and no chloritic or carbonate alteration was noted. Near the granite contact, the unit is cut by less than l m wide discontinuous aplite dykes and veins.

The Moira Lake granite, which intrudes the sedimentary sequence, underlies the southern shore of the large east-west trending swamp. As mentioned above, detailed mapping revealed that the granite is not as continuous across the southern portion of the property as Hewitt (1968) believed it to be. The south-central portion, that was originally mapped as granite, is actually an embayment of massive pelitic sediment within the granitic unit. The granite does exist as a continuous body, but only to the south of the property.

The granite is generally massive in outcrop, is cut by thin aplite dykes less than 2 m wide and has a thin gneissic outer mantle as illustrated on Map 87-57-01 (in map pocket). The outer gneissic mantle represents a zone of increased metamorphic alteration and tectonic movement parallel to the granite contact. This outer mantle is classified as an orthogneiss as it is derived primarily from the granite itself and contains only rare and thin discontinuous bands of biotite-rich material, believed to be recrystallized pelitic xenoliths.

The contact between the gneissic granite and the pelitic sediments is sharp, as revealed in drill hole MDR-87-1. Surprisingly, there was no evidence of

DERRY, MICHENER, BOOTH a WAHL

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Dcontact metamorphism within the metasediment in direct contact with the granite. There is, however, evidence of lower grade metamorphism of greenschist facies reflected in weak chloritic alteration and fine-grained muscovite development near the contact, within the pelitic metasediment.

Late Precambrian ultramafic sills or dykes intrude the complete stratigraphic sequence north of the granite. These units tend to be less than 3 m wide and range in composition from fine to medium-grained diorite to coarse- grained gabbro. Although there is minor contact metamorphism associated with these units, they do not play an important role in the formation of talc.

The Precambrian rock units are overlain unconformably by an Ordovician basal conglomerate. These outliers have been noted in three areas of the property; the eastern margin of the north half of the mapped claims; between S.L. 1+OOE and 1+25E roughly 60 m north; and as a thick wedge underlying the swamp as revealed by drill hole MDR-87-1. Although some outliers of this material were anticipated, the thick wedge underlying the swamp was not. Drill hole MDR-87- 01 intersected the basal conglomerate from 109.59 m to 164.63 m at a vertical depth from 80 m to 115 m (Figure 6).

\The position and vertical extent of this material and the shearing and

intense microfolding noted in the Precambrian rocks near the shores of large east- west trending swamp suggests that some large scale tectonic feature, such as an extensive fault system, may exist underneath the swamp, possibly paralleling the contact of the granite.

Structural Geology

Although all the units on the Moira Lake property have undergone intense folding and some shearing during the Grenville Orogeny, not all units give evidence of this regional tectonic event. The massive marbles generally do not show any evidence of folding or shearing as these units may be completely

_) recrystallized. However, the interbedded pelitic material within the marbles and


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ythe true metapelite units often appear intensely folded and show evidence of weak to moderate shearing.

The large northeast trending swamp is believed to be underlain by an extensive fault system. This is postulated due to the evidence found in outcrop on both the northern and southern shores of the swamp and from drill core.

On the northern shore intensely folded pelitic beds exist within the marble sequence. Due to the readiness of carbonates to recrystallize, the intense deformation is only reflected in the pelitic interbeds, but it is clear that the entire sequence has undergone a high degree of deformation. The folding is tight to isoclinal with fold axis trending roughly 070O and plunging steeply towards the southwest between 75 0 and 800. The limbs of the folds are overturned and dip steeply towards the north-northwest between 80 O and 85O. The orientation of this folding is similar to that found by Hewitt (1972) at the Cantal Mine site. This similarity is encouraging in that the folding at both the mine site and the property may be related to the same deformational event.

Weak to moderate shearing is found along the southern shore of the swamp within the metapelites and along the outer mantle of the granite, as evidenced in outcrop and in drill core. Generally, the shear intensity increases towards the granite contact, although moderate shearing is also found along the southern shore of the swamp in the south-central portion of the property, where the massive pelitic unit exists, as illustrated in Map 87-57-01 (in map pocket). This shows that the shearing along the southern shore of the swamp is not caused by the intrusion of the granite, but rather related to the large scale faulting that is thought to exist underneath the swamp.

Further evidence to this faulting is given by the thick wedge of Ordovician sediments that was intersected in drill hole MDR-87-1 from 109.59 m to 164.63 m at a vertical depth from 80 m to 115 m, as shown on Section 5+OOE (Figure 6). Since this Ordovician material lies unconformably on top of the Grenville rocks, a large fault block or fault zone must exist under the swamp to allow such exaggerated basement relief.

DERRY, MICHENER. BOOTH a WAHL

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TfflN SECTION ANALYSIS

A total of 40 rock samples in three separate groups were selected from outcrops, trenches and diamond drill core. The samples in Groups I and li were taken along two roughly parallel lines along the western margin and the central portion of the property, respectively, to locate any existing reactionary trends within the dolomites. Group II also includes 9 samples of drill core from Hole MDR-87-1 {DC Series). The samples in Group III were taken from various outcrops across the property as an aid in rock identification. The samples in each group are listed as follows:

GROUP I (Western Margin)

GROUP II (Central Portion)

JJM 28JJM 29JJM 24JJM 25JJM 27JJM 43JJM 45JJM 53JJM 51JJM 46 ^JJM 35JJM 38JJM 50JJM 36JJM 49

15

JJM 14T 523T 502T 524JJM 17JJM 19JJM 60JJM 55JJM 58JJM 57JJM 21DC 01DC 03DC 04DC 05DC 07DC 08DC 13DC 15DC 16

GROUP mJJM02 JJM 03 JJM 06 JJM 07 JJM 09

20

Sample locations are shown on Map 87-57-01, Figures 5 and 6. Detailed thin section reports and a summary by Geoprocess Consulting Ltd. are given in Appendix III.


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DISCUSSION

Thin section analyses revealed that most of the samples selected in Groups I and II are composed of medium- to coarse-grained dolomite with uniform mosaic texture. Many of these sections show signs of recrystallization with a general decrease in size and rounding of individual grains. Similarly, rounded quartz grains were also noted in many of the recrystallized sections but reactions betweeen the individual quartz and dolomite grains were not noted.

Talc and related tremolite were found in several sections from the Group I samples, as listed below:

ample Number

JJM 43JJM 53JJM 46JJM 50JJM 49

Talc

X

X

x

Tremolite

X

Xx

Although no reaction trend was noted along the sampled line of Group I, the presence of the talc and tremolite is encouraging. The Group II samples were devoid of talc or tremolite; however, minor talc was identified in two of the Group III samples.

Since talc and tremolite crystals were noted in only a few of the Group I sections, future work should focus on the western margin of the property. As abundant quartz veining and some tremolite formation was also noted during the surface mapping, this area is of particular interest.

CONCLUSIONS AND RECOMMENDATIONS

Surface mapping, trenching and diamond drilling revealed that the Moira Lake property is underlain by the same northeast trending, intensely folded sequence of dolomite and metapelites as found at the Cantal mine, 2 km to the


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west. A detailed thin section analysis of a number of samples selected from the property found that talc and tremolite have formed at some locations, although reaction trends along samples lines were not noted.

Although the Phase I exploration program did not locate significant talc mineralization within the dolomitic sequence, a large portion of the property, underlying the northeasterly trending swamp remains uninvestigated. In addition, west of drill hole MDR-87-1 quartz veining within the dolomitic sequence becomes more intense and large tremolite crystals have been found; the presence of both these minerals is encouraging as they typically occur in the wallrock of talc deposits. It is therefore possible that talc formation may have occurred, in association with the quartz and tremolite, in rocks under the northeast trending swamp or at depth. A Phase II followup drilling program is recommended that focuses on the area west of the present drill hole under the large swamp to test the former possibility.

PROPOSED PROGRAM AND BUDGET

A two-part Phase II followup diamond drilling program is recommended for the Moira Lake Talc property. Each of the two parts of Phase II will consist of 1,500 ft. of diamond drilling for a total footage of 3,000 ft.

The first part of Phase II will consist of three shallow holes underneath the swamp. The location, orientation and length of the proposed holes is as follows:

Diamond Drill Hole

MDR 87-2 MDR 87-3 MDR 87-4

Location

N.L.3*OOE;2*70S N.L.H-75E;3*40S N.L.O+25EJ4+40S

Azimuth Dip Length

160016001600

-450S-450S-450S

500 ft. 500 ft. 500 ft.

1,500 ft.


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Contingent upon favourable results from Part l, the Part 2 portion of Phase II will consist of an additional 1,500 ft. of diamond drilling to be located based on results from the Part l drilling. This drilling will consist of additional shallow holes or possibly a deeper hole under the Part l holes.

The total estimated cost of the Phase II program is S105,000 as follows:-

Phase II

Part l - Diamond Drilling1,500 ft. @. approx. S32Xft. incl. supervision, assays, etc.

Part 2 - (contingent)1,500 ft. @. approx. $32/ft. incl. supervision, assays, etc.

Total

Contingency - approx. 1096

GRAND TOTAL

48,000

48.000

S 96,000

9.000

SIOS.OOO


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REFERENCES

Ehlers, E. G. and Blatt, H. 1982: Petrology; Igneous, Sedimentary

Hartwick, P. A. and Woolham, R. W.1986: Report on the Moira Lake Talc

and Metamorphic; p. 625-631.

Prospect, Madoc, Ontario, N.T.S.31C/11, Prepared for Maradona Resources Inc., DMBWunpublished report, 25 pp.

Hewitt, D. F. 1968: Geology of Madoc Township and the North Part of Huntingdon

^—^ Township, Ontario Department( j 73, 45 pp., incl. ODM Map 2154.

of Mines, Geological Report No.

1972: Talc in Ontario; Ontario Department of Mines, Industrial MineralReport No. 40, 52 pp.

Simandl, G. J. and Ogden, D. G.1982: Industrial Mineral Potential of

Deposits, Madoc, Ontario;Unpublished report.

\

rtPBBV Ulf^LJE'klC'B BySSNYLJ Jfc

the Exceptional, High-Grade Talc Canada Talc Industries Ltd.

UIAUI

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CERTIFICATE OF QUALIFICATION

I, Jens J. Meyer, of 101 Donwoods Drive, Toronto, Ontario, do hereby certify that:

(1) I am an exploration geologist working as an outside consultant for Derry, Michener, Booth le Wahl, Consulting Geologists and Engineers, of Toronto.

(2) I am a graduate of Brock University, St. Catharines, Ontario, in Honours Geology, with the degree of B.Sc. in 1985.

(3) I have been practising my profession since 1984 and full-time since graduating in 1985.

(4) I have not received, nor do I expect to receive, any interest, directly or indirectly, in the properties or securities of Maradona Resources Inc.

(5) The statements contained in this report and the conclusions and recommendations made are based upon my review of all data available. I supervised and visited the property during the exploration program.

(6) I hereby consent to the use of this report in a Statement of Material Facts of the Company for the preparation of a prospectus for submission to the Ontario Securities Commission and other regulatory authorities.

-J

J. J. Mayer, B.Sc.

Toronto, Ontario J fl July 15, 1987 7 '

DERRY, MICHENER, BOOTH A WAHL

- 21 -

CERTIFICATE OF QUALIFICATION

I, Perry A. Hartwick, of 3500 South Millway, Unit 56, Mississauga, Ontario, do hereby certify that:-

1. I am an exploration geologist employed with Derry, Michener, Booth 4 Wahl, Consulting Geologists and Engineers, of Toronto.

2. I am a graduate of the University of Toronto in Honours Geology with the degree of B.Sc. in 1983.

3. I have been practising my profession since graduation.

4. I have not received, nor do I expect to receive, any interest, directly or indirectly, in the properties or securities of Maradona Resources Inc.

5. The statements contained in this report and the conclusions and recommendations made are based upon my review of all data available. I supervised and visited the property during the exploration program

6. I hereby consent to the use of this report in a Statement of Material Facts of the Company for the preparation of a prospectus for submission to the Ontario Securities Commission and other regulatory authorities.

Perry A. Hartwick, B.Sc

Toronto. Ontario o ' *O

l

Toronto, Ontario July 15, 1987

DERRY, MICHENER BOOTH ft WAHt

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APPENDIX I

ROCK DESCRIPTIONS

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APPENDIX I

ROCK DESCRIPTIONS

ORDOVICIAN

Sedimentary Rocks

lla - Basal Conglomerate

Tan to dark reddish- brown, fine-grained, equigranular, arkose matrix with 1096 to 3096, l cm to 20 cm, angular to subangular "sugary" white to light grey quartz clasts. Unit is massive in outcrop with only faint bedding visible locally. The dark reddish-brown colour is caused by strong hematite staining, which persists throughout. No alteration visible in hand sample, (see Plate 6).

lib - Argillite

Alternating very thin bands of medium to dark grey/green and reddish/brown, very fine-grained, strongly bedded argillite. Strong hematite staining throughout.

PRECAMBRIAN

Plutonic Rocks x

9a - Granite

Light pink to pinkish-grey, medium-grained, crystalline granite composed of mainly albite and quartz with minor microcline. Unit is massive in outcrop with minor weak jointing visible locally. No alteration visible in hand sample.

9a - Orthogneiss (Gneissic Granite)

Alternating thin discontinuous bands of tan to pink, fine-grained, highly siliceous and felsic orthogneiss. Unit exhibits strong gneissosity throughout with only rare occurrences of weakly banded material. Some more mafic looking, biotite-rich, discontinuous bands exist locally.


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9b - Aplite

Tan to pink, very fine-grained, highly felsic and siliceous aplite. Unit is massive in outcrop with only a very weak foliation visible locally. No alteration visible in hand sample.

7 - Diorite and Gabbro Undifferentiated

Dark olive green, medium- to coarse-grained, massive, mafic to ultramafic intrusive. Unit is generally weakly fractured with only very thin white carbonate material infilling. 196 to 296 pyrite as fine-grained disseminated material and in small concentrated blobs throughout. Weak to moderate chlorite alteration throughout and weak carbonatization locally. Weak foliation developed near contacts.

7a - Gabbro

Dark olive-green to black, medium to coarse-grained, massive, ultramafic intrusive. Coarse-grained pyroxene crystals visible in hand specimen. Very weak chloritic alteration throughout. Very weak foliation developed at contacts.

Metasedimentary Rocks

5 - Pelite

Dark grey to black, very fine-grained sediment. Unit is generally massive with only very faint bedding visible on weathered surface. Locally, the pelite is weakly fractured at random angles with very thin white to creamy-white carbonate material infilling. Very weak chloritization and carbonatization locally.

5 - Sheared Argillite to Phyllite

Dark grey to black, very fine-grained, weakly to moderately bedded argillite to phyllite. Unit exhibits weak to moderate shearing with fine* grained biotite and/or muscovite flakes developed along bedding planes. Minor interbedded very fine-grained and thin white carbonate-rich laminations. Very weak chloritization locally and weak carbonatiziation throughout.

5a - Dolomitic Pelite

Medium to dark grey, fine-grained strongly bedded dolomitic sediment. Unit contains 1096 to 2096 fine-grained white dolomitic carbonate material as thin laminations and disseminated material throughout. Very rare, fine-grained biotite flakes and medium to coarse-grained bladed kyanite crystals along some bedding planes. Very weak carbonate reaction only when scratched, indicating dolomitic carbonate.


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5b - Calcitic Pelite

Medium to dark-grey, fine-grained, well bedded calcareous sediment. Unit contains 1096 to 2096 fine-grained white calcitic carbonate material as thin laminations and disseminated material throughout. Locally very weak chloritization and fine-grained biotite flakes developed along bedding planes. Moderate to strong carbonatization throughout.

5c - Paragneiss

Dark grey to black, fine to medium-grained, banded paragneiss. Unit is composed of alternating discontinuous bands of dark biotite-rich and light grey crystalline siliceous material. Some small discontinuous bands of pinkish felsic material exists locally. Some zones of less metamorphosed material exist and are composed of mainly fine-grained biotite. These zones appear to be a transitional phase between the phyllite and the paragneiss.

4a - Dolomitic Marble

Tan to white, fine to medium-grained crystalline dolomitic marble. Unit is massive in outcrop with only faint bedding visible locally (see Plate 2). Depending on location, the dolomitic marble may contain thin discontinuous calcite stringers, discontinuous quartz veins and blobs and very thin reddish rhodocrosite stringers. Rarely, the unit contains fine to medium-grained, pale-green tremolite crystals and stromatolitic banding. Very weak reaction to acid only when scratched.

4ap - Pelitic Dolomitic Marble

Light to medium grey, fine to medium-grained crystalline dolomitic marble with minor interbedded and disseminated very fine-grained pelitic material. All other characteristics the same as the pure dolomitic marble.

4b - Calcitic Marble

Tan to white, fine to medium-grained crystalline calcitic marble. Unit is massive in outcrop with only faint bedding visible locally. Depending on location, the calcitic marble may contain thin discontinuous calcite stringers, discontinuous quartz veins and stringers and very thin reddish rhodochrosite stringers. Locally, the unit contains medium to coarse- grained euhedral calcite crystals. The weathered surface can be very irregular as quartz veins and stringers are more resistent than their host to weathering and the unit also contains deeply exsolved cavities. Stromatolites visible on weathered surfaces in some areas.


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4bp - Pelitic Calcitic Marble

Light to medium grey, fine- to medium-grained crystalline calcitic marble with thinly bedded and disseminated very fine-grained pelitic material. Where the pelitic material occurs as very thin interbeds, intense microfolding can be recognized in outcrop (see Plate 7). In these intensely folded areas, the pelitic material has largely been recrystallized to very fine-grained biotite. Where bedding is not apparent, disseminated pelitic material is recognized by the grey colour in hand specimen. As in the pure calcitic marble described earlier, this unit may contain calcite stringers, patchy coarse-grained calcite crystal development and very thin rhodochrosite stringers.

4c - Lime Silicate Rock

Tan, pink to light grey, moderately to strongly bedded, very fine-grained to fine-grained calcareous sediment (see Plate 5). The various colour changes within the unit are due to the clastic material incorporated in the rock. Generally, the "silicate" portion of the rock is fine-grained arkose material giving the rock a tan to pink colour. The grey areas are the result of minor disseminated pelitic material. Locally, the unit contains l cm to 5 cm stretched quartz stringers and/or clasts; fine-grained muscovite flakes developed along bedding planes; and arkose sediment dominated interbeds. Very strong reaction to acid throughout.

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DERRY, MICHENER, BOOTH A WAHL

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APPENDIX H

PHOTOGRAPHS OF TRENCHES, ROCK TYPES AND STRUCTURE


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Plate #2: Massive nature of thick marble sequence.

Plate #3: Dark grey and black pelitic marble within thick marble sequence.

Plate #4: Interfingering nature of "clean" white marble with dark grey pelitic marble.

Plate #5: Strong bedding found in lime silicate rocks.

Plate #6: Unconformable Ordovician basal conglomerate.

Plate #7: Intense folding found in pelitic marbles.

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Plate #1: Trench 325E (facing south),

Plate #2: Massive nature of thick marble sequence.

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Plate #3: Dark grey and black pelitic marble within thick marble sequence.

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Plate #G: Unconformable Ordovician basal conglomerate.

Plate #7: Intense folding found in pelitic marbles.

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APPENDIX m

TfflN SECTION ANALYSIS AND SUMMARY

BY GEOPROCESS CONSULTING LTD.

DERRY, MICHENER, BOOTH a WAHL

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Ill-1

TfflN SECTION ANALYSIS AND SUMMARY

SUMMARY

The series of rocks and drill core examined in thin section consists essentially of banded carbonate, almost entirely of dolomite composition. There are two exceptions, the one being JJM 07 which is pegmatitic in origin and mainly quartz having a cataclastic texture together with feldspar grains, a mixture of plagioclase and microcline accompanied by coarse muscovite flakes. The pegmatite suggests an intrusive introduced along the general foliation of the rock. This pegmatite has been brecciated and has cataclastic texture developed as the result of intense tectonic effect. This may follow a fault zone but doesn't follow any distinct faulting.

The dolomite is the predominant rock and shows considerable variation. Mostly it is medium to coarse grained having a reasonably uniform mosaic texture. This texture is modified in a number of ways suggesting the effects of shear zones or zones of stress. This modification results in the development of sugary texture in which the dolomite becomes much finer in grain and the mosaic pattern is changed to rounded grains in zones, producing a pattern-like string of beads, and the grain size is variable along the strings. Frequently the dolomite in these zones is accompanied by fine grained quartz.

The series of rocks is remarkably devoid of talc or even of serpentine or of asbestos. Antigorite is conspicuous by its absence in these rocks.

GROUP I

Section JJM 28

The rock is a very fine grained mosaic of dolomite. With the exception of one crosscutting veinlet composed of dolomite, the rock is featureless. The relationship between the veinlet and the matrix is not evident. Three grains of muscovite are present (approx. 2 microns in size), however no reaction with the dolomite is evident. These grains sit as isolated grains in the matrix.

Section JJM 29

This rock is similar to JJM 28 (very fine grained mosaic of dolomite). This rock is also essentially featureless except for a tendency of the dolomite grains to be ovoid and for the grains to align themselves accordingly. The few grains of quartz and muscovite are stable.


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Section JJM 24

This is a fine to medium grained carbonate with three grains of quartz and one of muscovite. No reaction is evident between quartz and dolomite. The muscovite sits in the dolomite matrix with no reaction and no apparent relationship to the dolomite.

Section JJM 25

Medium to fine grained carbonate - probably dolomite with about six grains of quartz in other minerals. (There are two sections with this number; both are similar and both show some mechanical breakup.)

Section JJM 27

The rock is mainly medium grained carbonate - probably dolomite. Slightly coarser grain size than in sections 28, 29 and 24. The grain is in a mosaic with somewhat preferred orientation. There are small patches of clusters of about ten each of the quartz grains not accompanied by any magnesium silicate grains. The total percentage of quartz is less than one percent.

Section JJM 43

This rock is a medium to coarse grained carbonate. Approximately twenty grains of quartz are present with each of them showing corrosion outlines resulting from reaction with the dolomite. Only three grains of talc are in the section. These grains were randomly positioned adjacent to grains of quartz and showed no sign of any genetic relationship to either the quartz or dolomite. The talc appears as stable blades with a thickness of 0.5 microns.

Section JJM 45

Fine grained granular carbonate as in JJM 28 with a tendency to the development of mosaic texture. Some rounded quartz grains - in the entire section thirteen quartz grains. No magnesium silicates - no minerals other than dolomite or quartz.

Section JJM 53

In this section tremolite occurs as bladed crystals enclosed in coarse grained carbonate. The tremolite is iron free and shows no signs of reaction rims or alteration (Plate 4). Frequently the tremolite is accompanied by a pale brown phlogopite. It occurs either randomly distributed as masses of flaky material or frequently in fractures within the tremolite.


III-3

Minor amounts of diopside appear as subhedral inclusions in carbonate not obviously related or associated with quartz of any of the tremolite or other magnesium silicates. The diopside does not occur in the tremolite.

Section JJM 51

Medium grained granular carbonate with no sign of mosaic texture. Dolomite with about ten grains of quartz. No other minerals visible; no signs of magnesium silicates present.

Section JJM 46

This is a medium grained carbonate with considerable brecciation of the dolomite. Quartz is present in minor amounts and displays a sugary texture (Plate 1). No reaction between the quartz and the dolomite is evident.

A few grains of talc occur alongside some of the quartz grains and associated with one quartz veinlet. The talc appears stable, however no genetic relationship with either the quartz or dolomite is evident. The association of talc with these minerals is a spatial one, with talc displaying the characteristics of random positioning. One single grain of diopside occurs in the section. It appears stable and only spatially related to the quartz and dolomite.

Section JJM 35

Medium grained carbonate - dolomite with mild brecciation; about two patches of fine grained quartz grains. Patches contain ten to fifteen quartz grains.

Section JJM 38

Medium to fine grained mosaic of dolomite with some zones of brecciation. About one to two percent medium quartz in the zones of brecciation - no magnesium silicates.

Section JJM 50

This rock is composed of a mosaic of medium grained dolomite with minor brecciation. Quartz occurs as either fine grained stringers or within patches of medium grained rounded grains within the dolomite. The one blade of iron free tremolite in the section is enclosed within the dolomite as a stable grain (Plate 3). No apparent relationship is evident between it and the dolomite and quartz. The few grains of muscovite appear as isolated grains in dolomite and display no apparent relationship to either the dolomite or quartz.


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Section JJM 36

Fine to medium grained carbonate - dolomite with a band of coarse dolomite. A few - less than two - very small grains of quartz. A few scattered grains of phlogopite. No other magnesium silicate.

Section JJM 49

Very fine grained dolomite carrying patches of fine grained sugary quartz. A few stringers of fine grained quartz occur throughout the slide. Adjacent to one of the stringers are two euhedral crystals of needle-like tremolite (Plate 2). The tremolite is stable and appears to be an inclusion within the dolomite. It also shows a rim of needle-like tremolite between itself and the quartz.

The six grains of talc in the section display the characteristic random distribution within the dolomite. The grains are stable and give the appearance of no genetic relationship to the surrounding dolomite.

GROUP n

Section JJM 14

Coarse carbonate mosaic - dolomite with occasional quartz grain and a few (plus or minus t en) xf lakes of muscovite. No magnesium silicates.

Section TS 23

Banded carbonate - dolomite, alternating bands of coarse mosaic and fine grained granular carbonate - a few - about six or eight grains of quartz and twenty or so flakes of muscovite.

Section TS 02

Coarse carbonate mosaic - dolomite partially replaced by medium grained sugary quartz but showing no reaction. No sign of magnesium silicates.

Section TS 24

In a small patch of sugary medium grained quartz there is a strangely isolated mass of five flaky antigorite grains associated with the quartz. There is probably a genetic relationship between the quartz and the antigorite as it seems to have a faint coloured rim against the quartz. There may be a genetic relationship to the surrounding dolomite but this relationship is not definite. The antigorite carries no talc.

DERRY, MICHENER, SOOTH ft WAHL

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" HI - 5

Section JJM 17

Fine grained granular dolomite in alternating bands of coarse mosaicdolomite with scattered small grains of muscovite. No grains of magnesiumsilicate. No quartz grains.

Section JJM 19

Coarse mosaic dolomite with some stringers of fine granular dolomite.The occasional grain of fine granular quartz but no magnesium silicates.

Section JJM 60

Very fine sugary dolomite with some small stringers of fine grained sugaryquartz. No magnesium silicate, some patches of dirty dolomite with fine grainedfibrous abestos. No significant amount of magnesium silicate.

Section JJM 55

Rock is a fine grained mosaic of dolomite, with about five percent ofmuscovite in randomly oriented flakes. There are a few patches of brecciateddolomite. There are a few ragged looking quartz grains associated with thebrecciated dolomite. No talc visible.

\

Section JJM 58

Medium grained sugary dolomite with occasional quartz grain and someclusters of quartz grains. No sign of magnesium silicates.

Section JJM 57

Medium grained sugary dolomite, occasional quartz grain. A few euhedralmuscovite. No magnesium silicates.

Section JJM 21

Medium grained granular dolomite with medium grained granular quartzirregularly distributed. A few tabular muscovite flakes. No magnesium silicates.

DERBY, MICHENER, BOOTH ft WAHL

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III-6

The following nine sections are from drill core.

Section DC 01

Uniform grained medium to fine grained mosaic of dolomite with very occasional rounded grains of quartz. No sign of magnesium silicate.

Section DC 03

Medium grained mosaic of dolomite grains slightly coarser than DC 01. Small patches of rounded quartz - total about 0.596 to 196 randomly distributed. Occasional muscovite flake.

Section DC 04

Medium grained mosaic of dolomite grains randomly oriented with a few coarser grains of dolomite which are turbid and contain very fine grained dark material having the appearance of carbon. There are occasional muscovite flakes. No talc visible.

Section DC 05

This rock has the appearance of being the same as DC 04 but subjected to crush brecciation. Its consists of zones of very fine sugary grains arranged in zones sometimes of very fine grain. The zonal arrangement applies also to the turbid material which is drawn into a schlieren. Very few sugary grains of quartz.

Section DC 07

Medium to fine grained mosaic of dolomite cut by a series of parallel zones of very fine grained dolomite. These have the appearance of crush breccia bands which are parallel to subparallel and seem to be mylonitic. Some of these carry the black opaque material as in DC 04. There are occasional euhedral muscovite grains and scattered rounded fine quartz grains. No talc.

Section DC 08

Medium to fine dolomite consisting of fine granular dolomite and interstitial very fine grained mylonitized dolomite suggesting the tectonic appearance as in DC 07 carried to the extreme. Both DC 07 and DC 08 may be parts of a fault zone. No talc or quartz.


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III-7

Section DC 13

Material in this is almost identical to that in Section DC 07 and these three sections may be part of the same fault zone.

Section DC 15

Very well banded quartzitic schistose rock. It consists of fine grained sugary quartz which alternate with bands of tremolite and greenish (olive) biotite. The latter contains bands of high magnesium chlorite obviously breakdown of biotite. Magnetite is common in the biotite bands. The biotite is strongly oriented parallel to the bands but there are coarse muscovite flakes with random orientation.

The quartz zones are like the dolomite of sections DC 08 etc., in that it consists of medium grained bands alternating with very fine sugary bands. There are random grains of dolomite in this section. The rock is a quartz rich biotite- chlorite schist.

Section DC 16

The best description of this is that it consists of alternating bands that are similar to DC 15 and alternatively like DC 08. Similar texture quartz rich but devoid of biotite and alternating with dolomite rich bands.

GROUP ffi

Section JJM 02

Within a patch of antigorite carrying random rounded quartz grains there are approximately 30 flakes of talc. The talc is clear and apparently uncoloured and ranges in size from 2 to 50 microns in length. These flakes do not appear to constitute a significant mass. Both the antigorite and the talc are associated with quartz, however there is no obvious genetic relationship.

Section JJM 03

Massive carbonate mainly coarse mosaic with stringers of granular dolomite and evenly distributed granular quartz, the quartz amounting to about ten to fifteen percent as a fairly regular peppering of fine grains in elongated zones. This is accompanied by oriented muscovite flakes so that the rock has a shistose texture of muscovite parallel to the quartz stringers and the dolomite. The muscovite is in patches of flakes throughout the granular dolomite and

\ related to the structure produced by the quartz zone.


lllllllll1)lllllllll

m -s

Section JJM 09

The rock consists of very coarse grained dolomite with stringers of quartz and muscovite throughout. These stringers appear to be very fine grained breccia zones in the dolomite and may be related to stressed dolomite within a shear zone or fault. The muscovite occurs somewhat parallel to the breccia zone and is not related to the quartz. The quartz in the zone is egg-shaped and commonly 0.5 microns in size. Quartz also occurs as a filling of tiny reaction holes or voids within the dolomite, however no reaction with the dolomite is evident.

Following the breccia zone are flakes of talc within the dolomite ranging in size from 0.5 to 1.0 micron. These flakes are stable and appear to be randomly dropped within the dolomite. The genetic relationship of the talc to the dolomite is not readily evident. The massive dolomite along this crush zone follows a sigmoid pattern.

Section JJM 07

Pegmatitic material mainly quartz and feldspar. The quartz massive together with some medium to fine grained sugary quartz probably cataclastic in origin. The coarse quartz is definitely cataclastic with cataclastic texture. This quartz contains two phase fluid inclusions with large gas bubbles suggesting pegmatite origin. The material suggests chilled origin and is mainly microcline and sodic plagioclase. There are a few large flakes of muscovite. The section contains no carbonate or talc.

Section JM 06

Massive mosaic of dolomite with ten to twenty percent very fine sugary quartz as in JM 09. The quartz is in bands and intergranular stringers and the individual grains are rounded. The stringers are arranged parallel to a regional parallelism. There are no feldspars with the quartz but there are broad bands and lenses of sugary quartz. There are numerous flakes of muscovite randomly oriented.


l l l l l l l l l

Ill - 9

Plata 1. Photomicrograph of Section JJM 46. Medium grained dolomite with sugary quartz. Note the lack of reaction between the dolomite and the quartz. Width of field is l.OB mm.

l l l l l l l l lJ

Plata 2. Photomicrograph of Section JJH 45. Within a stringer of fine grained quartz COD within the dolomite CD) is a needle-like grain of tremolite CT3 . The tremolite has a fine rim around its grain boundaries which is not readily apparent in this photo. Width of field is 1.08 mm.

GEOPRDCESS CONSULTINB

l l l l l l l l l

Ill - 10

Plate 3. Photomicrograph of Section JJfl 50. Medium grained dolomite COD uiith bladed crustal of tremoliteCT). Width of field is l.OB mm.

l

l

l

l

l

l

l

l

l

Plata H. Photomicrograph of Section JJil 53. Coarse tremolite (T) and carbonate CO). In this sample tremolite is commonly accompanied by phologopite filling fractures within the tremolite CarrowsD. Width of field is 1.08 mm.

6EOPROCESS CONSULTING

APPENDIX IV

DIAMOND DRILL LOG

HOLE MDR-87-1


co-ORDS: S.L. 5+OOE. 2+15S DERRY, MICHENER, BOOTH A WAHLDIAMOND DRILL RECORD

HOLE No. MDR-87-1

AZIMUTH: 1 60o PROPERTY: Moira Lake Talc Project

CMP: -450S DRILL TYPE 4 SIZE Longyear 38 - B Q LOCATION: Madoc. Ontario

ELEVATION: DIP TESTS: 116.16 m -SO^ (not corrected) 45" (corrected) DATE STARTED: May 26, 1987233. 27 m -470S (not corrected) 43" (corrected) DATE COMPLETED: May 28, 1987

LENGTH: 233.27 m LOGGED BY: jens MaverSECTION: R+nflF, DATE LOGGED: May 29, 1987PURPOSE: TO investigate geology under swamp that trends through the middle* of the property.

^

FOOTAGEfrom

0.00

3.63

to

3.63

47.87(4a to4a minP)

DESCRIPTION

OVERBURDEN - B W casing removed.

- Creamy white, pink and very pale green.- Fine-grained, massive crystalline, dolomitic

marble .- Very homogeneous unit with only subtle gradual

colour changes.- Very faint bedding visible in places around

650 GA.- Very rare thin creamy white to pink calcite

stringers at random angles.- Weakly to moderately fractured at random angles

causing core to be blocky in some zones - somefractures show hematite staining.

- 27.00 m to 47.87 m unit contains small lightgray discontinuous "sugary" quartz blobs andstringers giving the core a mottled appearancewhere quartz blobs are more abundant.

- Patchy calcitic marble.- Generally no carbonization without scratching

although some small local interbedded calciticmarble exists.

- No visible talc or tremolite formation.- Lower contact sharp - contacts 7/640 CA.

SAMPLENo.

DC-01DC-02DC-03DC-04

FOOTAGEfrom

5.0025.0035.0045.00

to

5.1025.1035.1045.10

LENGTH

0.100.100.100.10

SHEET No.:l Of 7

HOLE No, ..-.

FOOT from

47.87

66.44

AGE to

66.44(5b)

71.66(7)

DESCRIPTION

- Alternating thin beds and bands of medium todark grey and white.

- Alternating thin beds! (-O cm wide) of veryfine-grained to fine-grained calcitic pelite.

- Strong bedding visible throughout.- Unit is weakly to moderately fractured increasing'in intensity towards lower contact.

- Fractures are filled with thin creamy white topink calcite.

- Small local zones of weak to moderate shearingand some tight micro folding visible from appro*.56.00 m to 58.00 m.

- Very minor fine-grained biotite and/ormuscovite developed at upper contact.

- Lower contact sharp and marked by an 18 cmwide quartz vein.

- Contacts: 640 7570 GAStrong bedding at: 50.00 m fi 680 GA

60.00 m 6 71s GAWeak to moderate local shearing at 610 GA.

ALTERATION

- Moderate carbonization. Minor fine-grainedbiotite and muscovite along bedding planes.

- Dark olive green.- Medium-grained massive diorite dyke or sill.- Weakly fractured with very thin quartz/

carbonate infilling.- 2S pyrite, very fine-grained, disseminated.

and in very small (X 5 mm) stretched clots.- Weak foliation visible throughout at 550 GA

more pronounced towards contacts.

ALTERATION

- Contacts: 57omo CA- Weak to moderate carbonization.- Weak to moderate chloritic alteration.

SAMPLE No-

DC-05

DC-06

FOOTtrnj-Lfront

50.00

68.00

AGE to

50.10

68.10

.

LENGTH

0.10

0.10

SHEET No.: 2 Of 7

HOLE No.:MDR-87-3

FOOT from

71.66

106. 00

107.40

AGE to

106.00(5b)

107.40(4b)

108.74(4bp to

CKNOD./

DESCRIPTION

- Exactly as earlier 47.87 m to 66.44 m.- Weak to moderate local shearing at 700 GA.- Moderate to strong bedding at:

75.00 ra @ 660 GA85.00 m 6 600 GA95.00 m @ 73 0 GA

105.00 m @ 63 0 GA

- Unit contains rare small calcite crystal filledvugs. s

- No micro folding visible.- Lower contact abrupt but not sharp.- Contacts: 72o ;64 0 GA.

- Creamy pink to red.- Medium-grained crystalline calcitic marble or

calcite vein - massive, no bedding visible.- Unit contains several small calcite crystal lined

vugs.- Lower contact abrupt, but not sharp.- Contacts: 64*V630 GA- Very high carbonization.

- Alternating very thin bands of medium grey andcreamy white.

- Alternating very thin laminations or bands(1-2 mm) of calcitic pelitic sediment (grey) andcalcitic marble or carbonate (creamy white).

- Patchy, very fine-grained muscovite development- Rare, very small calcite crystal filled vugs.- Lower contact abrupt but not sharp. .- Contacts: 63-V640 GA.- Bedding at 66 0 GA.ALTERATION- Ho carbonization.- Calcite recrystallization.- Weak, fine-grained muscovite development.

SAMPLE No.:

DC-07DC-08

DC-09

FOOT from

80.00100.00

106. 50

AGE to

80.10100.10

106.60

LENGTH

0.100.10

0.10

^••MhMBM^H^^

SHEET No.: 3 of 7

HOLE No.: .AW.ft-8.7.4

FOOT from

108. 74

109.59

148.17

AGE to

109.59(4b)

148.17(lla)

151.22(lib)

DESCRIPTION

- Creamy white to pink.- Same as earlier 106.00 m to 102.40 m.- Rare, very thin light grey pelitic bands at

700 CA.- Very high carbonization.- Contacts: 6407580 .- Weak banding at 70" CA.

- Dark red to brown with grey 1 white clasts.- Fine-grained, massive, equigranular arkose with

10^151 1 cm to 5 cm diameter angular to ssubangular quartz clasts.

- Very heavily iron stained.- Unit is not very competent - breaks apart

easily causing core to be ground up and missing- Quartz clasts not present after 133.00 m.- 141.50 m to lower contact hematite staining

becomes less intense - rare thin), zones with nohematite staining.

- Some weak bedding visible towards lowercontact .

- Lower contact sharp but is broken.- No carbonization.- Contacts: 580 /? CA.- Weak bedding at 143.00 m at 560 CA.

- Alternating, very thin, dark grey /green andreddish brown.

- Alternating, very thin bands ( 1 mm) ofmoderately sheared to schistose, very fine grained, dark reddish brown and dark grey/green sediment.

- Hematite stained throughout.- Unit originally very thinly laminated red and

grey laminated pelite.- Tight micro folding visible in places.- Core tends to be blocky due to schistosity.

SAMPLE No.:

DC- 10

DC-11

FOOT from

121.00

150.00

AGEto

121.10

150.10

LENGTH

0.10

0.10

SHEET No.: 4 of 7

HOLE No.: .

FOOT from

151.22

154. 76

158.07

164.63

AGE to

154.76(Ha)

158.07(lib)

164.63(lla)

167.86(4b rain p)

DESCRIPTION

ALTERATION

- Moderate to weak shearing at 64 0 GA.- No carbonization.- Moderate chloritization.- Contacts sharp but broken.- Contacts: ?/? CA.

- Dark reddish brown with mottled grey/white.- Exactly as earlier 109.59 m to 148.17 m.- No carbonization. s- Contacts: 7/640 CA.

- Alternating, very thin dark grey 1 green andreddish brown.

- Exactly as earlier 148.17 m to 151.22 m.- Moderate to high shearing at 420-630 CA.- Contacts: 64"7530 CA.

- Dark reddish brown with mottled grey /white.- Exactly as earlier 109.59 m to 148.17 m. - No carbonization.- Contacts: 530 7470 CA.

- Alternating, discontinuous, light grey and lightpink.

- Fine to medium-grained crystalline, calcitic marble to calcitic othogneiss?

- Minor pelitic material, disseminated and in thinbands.

- Very high carbonization throughout.- Rare, small calcitic crystal filled vugs with

pyrite growing on calcite crystals.- Core ground up near lower contact (incompetent

zone ) .

ALTERATION- Very high carbonization.- Contacts: 47*V63 0 CA.- Banding at 650 CA.

SAMPLENO- FOOTIfOW

AGE lo LENGTH

.

SHEET No:. 5 of 7

HOLE No.:MDR-87-J

FOOTfjjmtirwin

167.86

193.73

222.77

AGE lo

193. 73 (5b)

222.77 (5:ffc)

233.27 (9a^t)

DESCRIPTION

- Alternating, medium grey and white. - Exactly as earlier 47.87 m to 66.44 m. - Strong bedding at: 170.00 m 8 63 0 GA.

180.00 m. 9 680 GA.190.00 m . 9 650 GA.

- Contacts: 630 7520 GA.

- Alternating, dark grey/green and white. - Very thinly bedded to laminated very fine

grained argillite or pelite and minor carbonate. - Very rare and thin quartz stringers at random

angles throughout - rare larger ones to 10 cm. but no associated mineralization.

- Weak shearing parallel to bedding. - Lower contact abrupt, but not sharp.

ALTERATION

- Weak to moderate chloritization.- Very weak to weak carbonization. - Patchy weak sericization near top contact. - Unit almost looks like a phyllite in places. - Strong bedding at: 195.00 m 6 630 GA.

205.00 m 9 630 GA.215.00 m 9 64* GA.

- Weak to moderate shearing around 63" GA. - Contacts: 520 7590 GA.

-) Alternating bands of light and medium grey with rare pinkish bands.

- Strongly banded fine-grained crystalline orthogneiss ( 9a ^* ) .

- Highly siliceous unit with only very weak carbon! zation throughout .

- Gneissosity decreases in intensity towards lower contact.

- Strong banding or gneissosity at:225.00 m @ 640 GA230.00 m 8 620 GA

SAMPLE No.:

DC-13 DC- 14

DC-15

DC-16

FOOTtmnimifrom

170.00 190.00

200.00

230.00

AGE to

170.10 190.10

200. 10

230.10

LENGTH

0.10 0.10

0.10

0.10

SHEET No: 6 Of 7

HOLE No.: .MD.R-r8.77J

FOOT from

233.27

AGE lo DESCRIPTION

- Contacts: 590 /? GA.

END OF HOLE

x

SAMPLE No.:

FOOT from

AGE to LENGTH

SHEET No.: 7 Of 7

Ministry ofNorthern Developmentand Mines

3tC11SWe*16 a.1*671 MADOC

Ontario Ministere du Developpement du Nord et des Mines

900

January 25, 1988 Your File: 87-60Our file: 2.10671

Mining RecorderMinistry of Northern Development and Mines10 Wellesley Street East1st floorToronto, OntarioM4Y 162

Dear Madam:

RE: Notice of Intent dated January 6, 1988Geological Survey submitted on Mining Claims EO 921259 et al in the Township of Madoc

The assessment work credits, as listed with the above-mentioned Notice of Intent, have been approved as of the above date.

Please inform the recorded holder of these mining claims and so indicate on your records.

Yours sincerely,

W. R. Cowan, ManagerMining Lands SectionMines and Minerals Division

Whitney Block, Room 6610 Queen's Park Toronto, Ontario M7A 1W3

Telephone: (416) 965-4888

Enclosure: Technical Assessment Work Credits

ONTARIO GEOLOGiCAt: i

FEB B

RECEIVED

cc: Mr. G. H. FergusonMining tt Lands Commissioner Toronto, Ontario

Maradona Resources Inc. Suite 50067 Richmond Street W. Toronto, Ontario M5H 1Z5

Resident Geologist Tweed, Ontario

Ministry of ' Northern Development

MinesTechnical Assessment Work Credits

Ontario] D*teJanuary 6, 1988

File

2.10671Mining Recorder* Report of Workfco. 87-60

Recorded HolderMaradona Resources Inc.

Towmnlp orMadoc

Type of survey and number of Assessment days credit per cliim ng Claim

GeophysicalElectromagnetic.

Magnetometer.

Radiometric —

Induced polarization.

Other————-^

-days

.days

.days

.days

.days

EO-921259 921261-62

Section 77 (19) See "Mining Claims Assessed" column

20 Geological _______II——-^^—

Geochemical.

days

days

Man days

Special provision

Airborne Q

Ground g]

j~j Credits have been reduced because of partial coverage of claims.

[~1 Credits have been reduced because of corrections to work dates and figures of applicant.

Special credits under section 77 (16) for the following mining claims

10 Days Geological

EO-921260

No credits have been allowed for the following mining claims{~| not tufficiently covered by the survey Q insufficient technical data filed

The Mining Recorder may reduce the above credits if necessary in order that the total number of approved assessment day* recorded on each claim does not exceed the maximum allowed as follows: Geophysical - 80; Geologocal - 40; Geochemical - 40; Section 77(19) - 60.

rMinistry o*

,'Matural •ources

Ontario

Report of Work (Geophysical, Geological, Geochemical and Expenditures)

The Mining Act

Instructions: — Please/type or print. (TN/J,/— If number, of mlning*cflimr"iravlr*

exceed* space on this form, attach a list.Note: — Only days credit* calculated In the

"Expenditures" section may be enteredin the "Expand. Days Cr." column*.

— Do not use shaded areas below.

dress of Author (of Qeo-Technlcel report)

\Jini

Credits Requested per Each Claim in Columns at rightSpecie! Provisions

For first survey:Enter 40 days. (This includes line cutting)

For each additional survey: using the same grid:

Enter 20 days (for each)

Man Days .

Complete reverse side and enter total (s) here

Airborne Credits

Note: Special provisions credit* do not apply to Airborne Surveys.

Geophysical

- Electromagnetic

- Magnetometer

- Radiometric

- Other

Geological

Qeochemlcal

Geophysical

- Electromagnetic

- Magnetometer

- Radiometric

- Other

Geological

Geochemical

Electromagnetic

Magnetometer

Radiometric

Days per delm

20

Days per Claim

Days per Claim

Mining Claims Trawted (Lift In numerical sequence)

Expenditures (excludes power stripping)Type of Work Performed

Performed on Clalm(s)

Calculation of Expenditure Days Credits Total Expenditures

S -1-15

Total Days Credits

s

Instructions Total Days Credits may be apportioned at the claim holder's choice. Enter number of days credits per claim selected In columns at right.

Dete Recorded Holder or Agent (Signature)

^/r-jUyV J/-Certification Verifying Report of Work/

Total number of mining claims covered by this report of work.

1 hereby certify that 1 have a personal and intimate knowledge of the fact* set forth in the Report of Work annexed hereto, having performed the work or witnessed same during and/or after its completion and the annexed report is true.

Name and Postal Address of Person Certifying

""T!*v\t"T MrtLJ*/ e^i,', L. Utn- .pD P 'i r k Mo vyt CV . f rt /rt /l)

^T

o . (Q rtDate Certified ' f'Qrr' 3 r* / P-"^

tati 0 *. jH*L 2.&VCertHjed by (Signature)

f J A

Huntingdon Twp3)C1lSWeet6 2.10671 MADOC

Twp.

Hungerford Twp

(D M

LU

LEGENDHIGHWAY AND ROUTf No

OTHER ROADS

TRAILS

SURVEYED LtNf sTOWNSHIPS BASt LINES.ETC -LOTS MINING CLAIMS PARCELS. ETC

UNSURVEYED LINESLOT LINESPARCEL BOUNDARYMININGCLAIMS ETC

RAILWAY AND RIGHT OF WAY

UTILITY LINES -

NON PERENNIAL STREAM -

FLOODING OR f LOORtNC, "K.nTS

SUBDIVISION ORr.OMF-OSirS P L AN

RESERVATIONS

ORIGINAL SHOHfLlhit

MARSH OR MUSKEG

MINES

TRAVERSE MONUMENT

DISPOSITION OF CROWN LANDS

TYPEOFpOCUMfNr

PATENT Si,R F AC t ". V 1 ^ '.

sum ATI w.iiM i'.MINiNd "U,"' 1-

LEASE SUHFACl ft MtNING

sum ActMINING fll

LICENCE Of ']CCIJPA T 'ON

OWOER IN CnUNCH

HESEHVATION

CANCELLED

SAND S GRAVEL .

SYMBOL

m. e

oB BaT

OC

MOT l

SCALE 1 INCH 40 CHAINS

••OOO 9OOO

AREAS .WITHDRAWN FROM DISPOSITION

M.R.O. - MINING HIGHTSONLY

S.R.O. -SURFACE H IGHTSONLY

M.+ S . - MINING AND SURFACE R IGHTS

DHtfTipiiDn O rdmr M o O am DripQWTiDfi ^il*

'SFACE i*lGHT S RF5Ef*VA"ION ALONG 'HE Of ALL L*KfcS AND HIVERS.

•"-r\ C P M,Ei O ---'^

DATE OF ISSUE

JAN 2 2 1988

SOUTHERN ONTARIO MINING DIVISION

TOWNSHIP

MADOCM M.R ADMINISTRATIVE DISTRICT

TWEEDMINING DIVISION

SOUTHERN ONTARIOLAND TITLES/ REGISTRY DIVISION

HASTINGS

Ontario

Ministry of Ministry ofNatural Northern DevelopmentResources and Mines

MARCH 1987

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Documents