Reconnaissance Re-evaluation, Deschambault Lake North (Part of NTS 63L)1

R. Macdonald

Macdonald, A. (1993): Reconnaissance re-evaluation, Deschambault Lake north (part of NTS 63L); in Summary of Investigations 1993, Saskatchewan Geological Survey, Sask. Energy Mines. Misc. Rep. 93-4.

The Deschambault Lake area considered in this report lies in the southeastern part of the Glennie Domain, im­mediately west of the Tabbernor Fault. The area was mapped originally in the fifties and sixties at a scale of 1 :63,360 for the Saskatchewan Department of Mineral Resources by S.J.T. Kirkland (1958) and W.A. Padgham (1968).2 Mapping by Sibbald (1972) and Thomas (1988a, b, and c) just touch on the northern margin of the area. Since then, much of the surround­ing region has been remapped at more detailed scales, and new interpretations have been advanced.

The present study is a reconnaissance investigation in­tended to re-evaluate rock units, deformational history, and mineralization potential, in order to relate them to in­terpretations in the contiguous terrain. This information is also being incorporated in a revision of a 1: 125 000 scale compilation map (Macdonald, 1992). A secondary objective of the project is to test out a new computer­ized method of entering field data.

This summer, observations were made almost entirely at shoreline exposures during 14 traverse days. As the area had been very thoroughly mapped by the original authors, their original lithological contacts and even some of their structural data have been used in the new map with few modifications. Rock unit descriptions have been revised, and the map legend and interpretations are new. The investigated area comprises the northern part of Deschambault Lake and includes Deschambault settlement (population ca. 700) and the peninsula to the south, the main part of the lake to the east, Portage Bay, and the narrow Northwest Arm and Northeast Arm.

1 . Lithology3

a) Plutonic and Other Intrusive Rocks

Osklkebuk Complex: The main part of the Oskikebuk Complex in this area appears to comprise a plutonic mass of uniform hornblende-biotite granodiorite. A thin section from the centre of the pluton is fresh and con­tains about 20 percent potassium feldspar. The south­ern part of the complex, in the region of Crooked Bay, comprises a varied plutonic assemblage, including leu­cocratic (probably granitic) sheets and narrow "grey dykes· of dioritic composition.

Hidden Bay Pluton: The main mass is a medium- to coarse-grained granodiorite with about 10 to 15 percent potassium feldspar. Exposures along the eastern mar­gin at least are more varied and include (leuco)tonalite. The main rock is typically grey pink, the pink coloura­tion being due to irregular staining of the feldspars along microscopic alteration traces.

Pait Lake Pluton: The southern part of this pluton which outcrops in the area, is a distinctive coarse uni­formly-foliated rock identified in one thin section as a hornblende-rich tonalite. Biotite occurs irregularly in sheaves, and garnet is also present in places.

Deschambault Pluton (Padgham's Deschambault Post Pluton): The Deschambault Pluton is wholly exposed in the area, in a rounded outcrop area about 4 km in di­ameter. The pluton has been compared by Padgham to the Brownell Lake and Maynard Lake plutons to the west. The only rock in the area which is marginally clas­sifiable as granite, this pluton contains biotite and mus­covite, is medium to coarse grained, and not particularly porphyritic. The colour is speckled pink white, the pink colouration here also is due to alteration and staining mainly of the plagioclase feldspar. The northern margin of the pluton is cut by numerous pegmatitic segrega­tions and stockworks which appear to derive from the pluton itself.

Ellis Island Pluton: This pluton has been named from the island close by. It outcrops along the peninsula which forms the east side of the Northeast Arm and is probably the continuation of the pluton cut farther north by the Tabbernor fault (Elliott, this volume). Several ex­posures around the southeastern and southern margin were examined. The rock is generally a dark tonalite and every exposure visited contains distinctive round pod-like inclusions of calc-mafic material which are gen­erally conspicuously weathered out. These exposures have possibly only sampled the marginal zones of the pluton, as at an exposure farther north up the Northeast Arm, the rock is paler, uniform and free of inclusions.

Other Granitolds: Two-mica granitoid was recognized in a few exposures on the islands between the outcrops of the Deschambault and Portage Bay plutons. Micro­cline forms small phenocrysts, and other components in­clude deep toffee-coloured biotite and muscovite. The

(1) Saskatchewan Project A.12c was funded in 1993 under the Canada-Saskatchewan Partnership Agreement on Mineral Development 1990·95. (2) As most references to previous work will be to these two authors, they will not be repeated in the text. (3) Lithological descriptions in this section are not formal and are intended to highlight only the main features observed in the field.

Saskatchewan Geological Survey 67

rock is medium grained, very uniform and typically weathers grey. The pluton along the west shore of the Northeast Arm, mapped by Kirkland as 'gneissic grano­diorite" (Unit 6b), is very coarse grained and also con­tains toffee-coloured biotite, but no muscovite.

Mafic Rocks: These were observed on Ellis Island and other islands in the eastern part of the main lake. They are mostly coarse and massive hornblende-plagioclase rocks with relict igneous textures. Ultramafic rocks were not found.

b) Metasediments

Metasediments, of a range of compositions underlie the northern part of the Deschambault settlement peninsula and much of the main lake to the east. They are mainly uniform, fine-grained, quartz-plagioclase rocks. Red brown biotite varies from about 5 to 15 percent. Potas­sium feldspar is typically absent, but in some thin sec­tions occurs in patches comprising 2 or 3 percent, remi­niscent of alteration. The texture is typically uniformly granulose (cf. the "biotite granulites· described by Pyke, 1961a and b, 1966) and others. Foliation is indicated by biotite orientation, subtle grain size differences and lo­cal quartzose stringers.

The interaction of differences in original composition and strongly varying metamorphic grade has produced considerable and complex variations in the metasedi­ments. Given a suitable scale, some of these are map­pable and a detailed lithostratigraphic-metamorphic map could probably be constructed.

Psammitic wackes are typically uniform rocks with about 5 percent biotite, and local muscovite. In many ex­posures layering is inconspicuous, and the wacke could be mistaken for a fine-grained plutonic rock. Immedi­ately south of Deschambault settlement the rocks may be described as schistose gneisses.

Wackes of more pelitic composition, apart from contain­ing more biotite, commonly contain layers of porphy­roblasts composed of various combinations of staurolite, sillimanite, and quartz. Kirkland's Unit 2a "nodular biotite gneiss and schist" falls under this cate­gory. Honey-coloured staurolite crystals up to 3 cm long occur in packed schistose layers in several places, par­ticularly on the west side of the Deschambault penin­sula. Graphite forms up to 2 or 3 percent of one sample which shows prominent quartz-staurolite nodules (Sta. 142; UTM 616634, 6077715).4

Hornblende is a minor component locally. Its presence may denote a tuffaceous admixture to the sediment.

At the eastern bay of the Northwest Arm, the metasedi­ments are anatectic, containing significant quantities of pegmatitic melt leucosorne (Padgham's unit 4i; Kirk­land's Unit 4).

Andalusite schist and slate (Kirkland's Unit 2b) was ex­amined in the small bay of the main lake east of Ellis Is­land (Sta. 251; UTM 619719, 6084058). A previously un­mapped exposure was also found farther up the North­east Arm (Sta. 259; UTM 618683, 6093776).

c) Metavolcanic Rocks

Rocks of volcanic origin were only previously identified in the area in an isolated exposure at the north end of the Northeast Arm (Kirkland's Unit 1) and in the south­west at the opening to Crooked Bay.

The assemblage at Crooked Bay is mixed, ranging from felsic to mafic, and the rocks are strongly deformed. Al­though augen structure and quartz ribbons were ob­served to be prevalent, a volcanogenic protolith seems probable.

This summer, volcanic rocks were identified in several new places:

Twin Bays: Existing geological maps show a band of hornblendic and calc-silicate rocks which extends from the Southeast Arm through Twin Bays to Alsmith lake, in general following the northern margin of the Oskike­buk Complex. Padgham's Unit 5 was examined at the westernmost of the Twin Bays, on islands and the pen­insula across the main lake, and also along the road section to Deschambault Resort. The rocks vary from massive, medium-grained to banded and laminated am­phibolites comprising mainly plagioclase and horn­blende with subsidiary calc-silicate minerals. The Twin Bays exposures also show quartz ribbons. The Indi­cated derivation is by shearing from a volcanic protolith.

Northwest Arm: In these instructive exposures, a transi­tion was seen from attenuated but distinctly recogniz­able pillow lavas on a small island (Sta. 084; UTM 609903, 6097221) through strongly laminated calc-sili­cate amphibolites clearly derived from them by deforma­tion. Massive amphibolite believed to be derived from basaltic flows, and felsic to mafelsic gneisses also out­crop along the west shore of the Northwest Arm. The latter are uniform rocks with small garnets, highly flat­tened quartz eyes and quartz ribbons, and no potas­sium feldspar; both in field exposure and thin section they are similar to rocks elsewhere identified as de­formed dacitic volcanics.

Junction of the Southeast Arm: Massive amphibolite is well-exposed among the islands immediately west of the junction of the Southeast Arm with the main lake. Patches, discontinuous layers, and reticulated veins of calc-silicate material, occurring locally at intervals within the amphibolite, suggest interflow and other types of breccia and interffow selvage. A small island (Sta. 156; UTM 613231, 6078785) is made up entirely of rodded pillow structures in amphibolite. The pillows average about 25 cm in cross-section due to the stretching.

(4) Point locations are given in this report first by station nurrber and then by east and north UTM coordinates (Zone 13).

68 Summary of Investigations 1993

Here, as in a large cliff exposure on the north shore of another island in the main lake (Sta. 168; UTM 611932, 6081388), the selvages of the strongly rodded pillow forms are rusty and contain calc-silicate and sulphide minerals.

A strongly rodded felsic rock exposed in a nearby local­ity (Sta. 153; UTM 613996, 6078597) comprises coarse and fine plagioclase, patchy quartz, carbonate, a little chlorite, and up to 5 percent sphene crystals arranged in irregular trains. Attributed in the field, despite the de­formation, as a felsic volcanic, the thin section evidence suggests it is possibly an altered mafic volcanic.

d) Conglomerates

Conglomerates were mapped by Padgham in the west­ern part of the area between the Portage Bay and Deschambault Lake plutons, and have been recorded farther west towards Brownell Lake (Padgham, op. cit.; Delaney, 1988a, b, and c). They are exposed in rela­tively undeformed state at several places within the out­crop of the Hidden Bay Pluton. Two new features were observed this summer:

1) The conglomerates are generally very poorly sorted and contain a great variety of clasts from wide­spread geographical sources.

2) They have been observed in two places to be cut by granodiorite of, or associated with, the Hidden Bay Pluton.

The matrix is generally a grey, medium-grained grit. The clasts include granodioritic rocks in rounded cob­bles and boulders up to about 30 cm across, felsic and mafic fragments (some patently volcanic), vein quartz, ultramafic material, weathered calc-silicate rock, horn­blende-porphyritic rock, and rusty felsic rock. Apart from the rounded plutonic boulders, most clasts are angular to lensoid and generally not more than about 1 O cm long. What appear to be pelitic fragments occur pro­fusely in places, and are entirely matrix supported. The grit matrix could be mistaken at first glance for a me­dium-grained plutonic rock and the fragments for xeno­liths (cf. the Sykesville •granite"; Trzcienski et al, 1992; Hopson, 1964; Drake and Morgan, 1981), but they are undoubtedly fragmental sediment and more probably rip­up clasts. The mixture of proximal and distal clasts indi­cates derivation from emergent terrain for at least the rounded boulders, and sources close by for the angular clasts, probably under submergent conditions. Grano­diorite of Hidden Bay type cuts the conglomerate on the northeast shore of Portage Bay (Sta. 038; UTM 601605, 6088952). Apophyses of granodiorite about 5 cm wide and one metre long cul into the conglomer­ate including, significantly, across a boulder of an ear­lier granodiorite of similar appearance.

The stratigraphic position of the conglomerates has not been determined; they are probably intraformational with the greywackes, as considered to be the case far­ther west (Delaney, pers. comm.). This factor, together with their unsorted nature and highly divergent composi-

Saskatchewan Geological SuNey

lion and source, might justify their designation as diamictites.

e) Pegmatltes

Pegmatites of distinctive genre are abundant locally, and sorting them out would require further study. The following types were noted:

1. Stockwork and segregation muscovite-biotite pegma­tites are associated with the Deschambault Pluton. Pegmatites of similar composition, but of more sharp-walled form observed on neighbouring islands to the north may be related.

2. Melt-type pegmatitic feucosomes form up to about 10 or 15 percent of the outcrop of anatectic me­tasediments along the northeastern embayment of the Northwest Arm.

3. Sharp-walled pegmatites containing biotite and/or muscovite are abundant mainly among the metasedi­ments directly east of Tower Island. Some of these contain large masses of black schorl tourmaline (the largest observed is about 15 cm long).

4. A regularly-striking sharp-walled pegmatite up to about 6 cm wide on a small island near Tower Is­land (Sta. 242; UTM 609077, 6087482) contains what appeared to be very small beryl crystals.

5. Very large bodies of very coarse to fine pegmatite with inclusions of country rock occur along the east­ern side of the main fake and up the Northeast Arm (Kirkland's Unit 7a).

6. A wide outcrop of coarse muscovite-bearing migma­titic gneiss occurs on the east shore at the northern extremity of the Northwest Arm, and similar rocks were observed on Mcintyre island and the mainland immediately east (Kirkland's "biotite-muscovite quartz monzonite" Unit 7a).

2. Metamorphism

The area has been subjected regionally to the full range of amphibolite facies metamorphism, and lower grade metamorphism particularly along brittle-ductile shear zones. The complexity of the metamorphic pattern is ap­parent from marked variations in mineral composition to­wards the Tabbernor Fault zone, and among the me­tasediments of the Deschambault peninsula and the main part of the lake. An analysis of this pattern has not been made.

3. Structure and Tectonic Sequence

The metavolcanic, and possibly other supracrustal, rocks lying immediately alongside the northeastern flank of the Oskikebuk Complex are strongly sheared in a northeasterly dipping high-strain zone. This zone is ap­parently continuous with the Hartley Shear Zone, run­ning through Alsmith Lake to the west, which also forms

69

the northeastern flank of the Oskikebuk Complex (De­laney, 1988a}.

The northern margins of the Oskikebuk Complex also exhibit a strong north-northeasterly dipping foliation as well as north-northeasterly plunging lineations. As no significant indication of minor folding was observed, the linear fabrics are interpreted as stretching lineations. Similar linear fabrics were also recorded in the Brownell Lake area by Delaney {1988a}. Both the foliation and lineation largely die out into the centre of the complex, but partially pick up again along the southern margin in the composite intrusion zone underlying Crooked Bay. In the zone of supposed metavolcanics occurring imme­diately south, shearing is intense, with the same north­easterly dip.

The pattern of southwesterly-vergent stacked thrust sheets proposed for the southern part of the Glennie Domain (Lewry and Macdonald, 1988) appears, there­fore, to obtain also in this area.

The southwesterfy vergence is maintained in general throughout the remainder of the area, but is compli­cated by regional folding on north-south axes around Viney Lake, and by more northeasterly-plunging folds over the remainder of the area to the north. These folds are accentuated in the metasediments of the Descham­bault peninsula where they range in dimension from ex­posure to map scale. Primary layering and various sec­ondary cleavage fabrics, some axial planar, were re­corded by Padgham and verified by the writer both in field exposure and from photogeological interpretation. These folds might be labeled 02, at least for descriptive purposes (equating with Delaney's (1988a) 03 in the Brownell Lake area), and the southwesterly vergent structures of the Oskikebuk Complex as 01.

The disposition towards stretch L-fabrics observed in the Oskikebuk Complex is also shown by the strong north-plunging rodding in the pillow lavas and the al­tered falsie volcanics on islands in the main lake, and is probably present with less certain recognition in other units.

High-strain zones, which generally trend north to north­northeast, occur along all arms of Deschambault Lake, including the Southeast Arm (Macdonald and Posehn, 1976; Lewry, 1990) south of the present area.

Northwest Arm: Shearing occurs mainly on the west­ern shore, involving mainly volcanic protoliths. The shear zone affects the Pait Lake Pluton and may also bend around its southern margin. Padgham marked a brittle fault down the middle of the Northwest Arm and continued it south to Portage Bay. The conglomerates at Deschambault settlement are also highly strained on a northeasterly strike. This strain zone dies out rapidly on both sides of the settlement, and its relation to the Northwest Arm strain zone Is undetermined.

Northeast Arm: A very brief examination of this arm confirmed the presence of minor straight belt features such as occur in the "Pelican Slide" immediately to the east. The very large pegmatite bodies outcropping

70

along this arm also lie along the same strike, suggest­ing that their emplacement was controlled by the same tectonism. Later brittle-ductile shears of the type en­countered farther north by Elliott {this volume) were also found in the northern part of the Ellis Lake Pluton, close to Kirkland's outcrop of Unit 1 "basic volcanic flow rocks".

Chronology of the Late Plutons and Pegmatites: The Hidden Bay Pluton has been observed to intrude the conglomerates. As these are probably intraforma­tional with the metasediments and even with the meta­volcanics, it may be concluded that this pluton post­dates all supracrustals in the area.

Although the Deschambault Pluton possibly also post­dates the metasediments, intrusive relations are less certain. The granite was observed to intrude metasedi­ment in one place, but the exposure is small and the metasediment could be a large xenolith. Moreover, the country rock metasediments appear to be deformed around the rounded outcrop of the pluton.

The relation of the timing of emplacement of these late plutons to the linear high-strain zones has not been di­rectly determined, but on the general grounds that shear fabrics have not been encountered in them, it is suggested that they are later.

The large pegmatites along the Northeastern Arm were only visited at two locations and there found to be de­void of ductile shear fabrics. By their position along the high-strain zone it would seem they too might be post­shearing and could represent late annealing intrusions. Further observations in the area, particularly on the country rock inclusions, should be able to resolve this question.

4. Saprolitic Weathering Profile

Saprolitic weathering was encountered on the northeast shore of Portage Bay, in a protected position where pre­sumably the ice sheets failed to completely strip off the weathered material (Sta. 039; UTM 600506, 60887 41 ). The weathering is red, and was at first mistaken for a gossan, but no significant quantities of sulphide were found. The saprolite affects conglomerate, and because of this we were able to dig out an undeformed mafic boulder from the weathered gritty matrix.

5. Potential for Mineralization

The area contains a few old showings and three min­eral occurrences recorded by Padgham. Information is taken from the Saskatchewan Mineral Deposits Index (SMDI) and field observations.

Padgham's occurrences include SMDI 0271 (UTM 607789, 6095543) (chalcopyrite in "calc-silicate gneisses") and SMDI 0274 (UTM 615976, 6093274) (disseminated pyrite and flakes of graphite with traces of chalcopyrite) which occur on the west shore of the Northwest Arm. The occurrences were not located in the field, but the regional host rocks have now been

Summary of Investigations 1993

identified as sheared volcanogenic rocks, including pil­lowed basaltic flows and dacites.

Padgham also recorded another occurrence of pyr­rhotite and chalcopyrite, SMDI 0272, (UTM 612050, 6085164) on the same small island in the main lake where the writer identified pillow lavas.

Showing CBS 6225 (SMDI 0275; UTM 600577, 6091201): This showing was also found by Padgham and although staked much later, in 1986, by Odin Re­sources there was no outcome. At the showing, pyr­rhotite occurs in "hornblende, calc-silicate layers and lenses and in conglomeratic quartz-feldspar schist, gneiss and granulite". The context again may be vol­canic, with the addition of conglomerate.

Showing known formerly as the RAT claim No. 16 (SMDI 0276; UTM 607673, 6095168): This showing is also located on the west shore of the Northwest Arm, in the same volcanic environment as the other occur­rences so far described. Hudson Bay Exploration and Development Co. commenced work on this showing in 1955 with an airborne radiometric survey. This was fol­lowed up in subsequent years (through to 1983) by A.L. Parres with airborne EM and ground magnetic sur­veys, and a program of drilling was implemented. The drill holes intersected a zone of massive sulphides con­taining pyrite, pyrrhotite, and minor associated sphalerite.

Showing known formerly as the RAT Nos. 16 and 64 claims (SMDI 0270; UTM 610891, 6093764): This showing is apparently located in a different environment on the western bay of Northeast Arm. Here the regional host rocks are mainly metasedimentary, although the file does indicate the mineralization is hosted within "quartz-feldspar-garnet-hornblende gneiss". The show­ing was trenched and assayed at 0.53 to 1.0 percent Cu, 0.03 to 0.05 percent Ag, and traces of Mo. Dissemi­nated sulphides were also intersected in drill holes put down in the period 1965 to 1969.

In general terms, the recognition of the greater extent of volcanic precursors in the area than considered pre­viously, and the presence of high-strain zones should hold promise for further exploration.

6. Appendix: Digital Technology used in the Project

A procedure for entering geological data directly from the rock exposures was devised and tested for the pro­ject. This was achieved with a small hand-held "vest pocket" computer, and data were transferred each eve­ning to a PC in camp to a main database from where the geological map could be plotted.

Field data were entered directly in the field using a Ca­sio BOSS Organizer, Model SF-20. This computer folds

(5) Fieldlog was developed originally by the Ontario Geological Survey.

Saskatchewan Geological Survey

up and can be carried easily in one of the pockets of a surveyor's vest. A standard field mapping board was modified to serve both to carry the base map and pho­tos, and as a "desk" for the computer. Station locations were entered onto the base map or, along road sec­tions, were determined by means of a Magellan GPS in­strument and entered into the spreadsheet.

When researching available "organizer" sized comput­ers, it had been intended to find one with a programma­ble database function, but we could not find one at the time with adequate features, so we switched to entering data through a spreadsheet. The Casio BOSS SF-20 has a Lucid 30 spreadsheet with 256 columns, 9,990 rows and 256K of RAM, which is more than adequate for the task. Although there is enough space to hold several day's data and the files were maintained there for field reference purposes, for security reasons the data were also copied to the PC every day. The daily transfer was effected by means of PC LinkPlus soft­ware and its companion serial connection cable which connects the BOSS to the PC through a COM port.

The Lucid 30 spreadsheet files were transferred to the PC in WKS format and from there to a general data­base, in this case Q&A 4.0, where the data are main­tained. This option was chosen because of the ability of a general database to handle both the field data, includ­ing text, and other files, such as petrographic reports, etc.

The geological map was produced, as is our general practice these days, through the PC using the Field­Log5 version 2.83c provided by the Geological Survey of Canada, in combination with AutoCAD Release 12. Only the fields necessary to construct the geological map were copied from the database into Fieldlog. Ta­ble templates used in Fieldlog were modified to suit these inputs.

Geological data were then copied onto a compiled digi­tal base map produced from 1 :50 000 scale digital files provided by the Central Surveys and Mapping Agency, Saskatchewan.

The computer organizer performed reliably in the field, and was not backed up with a pencil and paper note­book, as only one day's data are at risk. The keyboard is small, but adequate for two finger typing. By entering data directly on the rocks, the need to re-enter data on the PC in the evening was eliminated. Other computer organizers are coming on the market, and doubtless this technique could be refined, particularly if these in­struments were to combine graphics and database op­tions. Such is the promise, perhaps, for the next genera­tion of Personal Digital Assistants (PDAs).

71

7. Acknowledgments

The writer wishes to acknowledge review of this contri­bution and helpful consultation with Gary Delaney for two days in the field. Brent Czornobay helped with the redesign of the Fieldlog tables to accommodate trans­fer of data into Fieldlog, and Irvine Gaw produced the modified field mapping board used in the project. An­drew Buchanan assisted in the field and undertook much of the base map compilative work.

8. References Delaney, G.D. (1988a): Bedrock geological mapping, Brownell

Lake ~re~ (part of NTS 63M-4 and 63L-13); in Summary of lnvest1gat1ons 1988, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 88-4, pB-19.

____ (1988b): Bedrock geology, Brownell Lake area (part of NTS 63M-4 and 63L-13); Sheet 1 : East; 1 :20 000 scale prelim. map with Summary of Investigations 1988, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 86-4.

____ (1988c): Bedrock geology, Brownell Lake area (part of NTS 63M-4 and 63L-13); Sheet 2: West; 1 :20 000 scale prelim. map with Summary of Investigations 1988, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 88-4.

Drake, A.A. and Morgan, B.A. (1981): The Piney Branch Com­plex-a metamorphosed fragment of the central Appala­chian ophiolite in northern Virginia; Amer. J. Sci., v281, p484-508.

Hopson, C.A. (1964): The crystalline rocks of Howard and Montgomery counties; in The geology of Howard and Montgomery counties, Maryland Geological Survey, p28-337.

Kirkland, S.J.T (1958): The geology of the Deschambault Lake area (east half), Saskatchewan; Sask. Dep. Miner. Re­sour., Rep. 31, 16p.

Lewry, J.F. (1990): Bedrock geology, Tulabi-Church lakes area: Derivation and significance of porphyroclastic gneisses in the Pelican Window; in Summary of Investiga­tions 1990, Saskatchewan Geological Survey, Sask. En­ergy Mines, Misc. Rep. 90-4. p36-43.

Lewry, J.F. and Macdonald, R. (1988): Observations on defor­mation in the Glennie Domain and Hanson Lake Block; in Summary of Investigations 1988, Saskatchewan Geologi­cal Survey, Sask. Energy Mines, Misc. Rep. 88-4, p35-41.

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Macdonald, R. (1992): Sheet 63L-NW, Pelican Lake and Amisk Lake Bedrock compilation Geology Series; Sask. En­ergy Mines, digital Open File Map 92-DOF1.

Macdonald, R. and Posehn, G.A. (1976): Limestone-Tulubi lakes (revision mapping), 63L-11 (E); 1 :50 000 scale map With Summary of Investigations 1976, Saskatchewan Geo­logical Survey, Sask. Dep. Miner. Resour.

Padgham, W.A. (1968): The geology of the Deschambault Lake district comprising the Oskikebuk Lake area, Viney Lake area (west half), the northern part of the Ballantyne Bay area, and the northeast quarter of the Limestone Lake area; Sask. Dep. Miner. Resour., Rep. 114, 92p.

Pyke, M.W. (1961a): 63-M-2-E: The Pelican Narrows area (east half); in Summary of Geological Surveys Conducted in_the Precambrian Area of Saskatchewan; Sask. Dep. Miner. Resour., p2-4.

____ (1961b): The geology of the Attitti Lake area (west half), Saskatchewan; Sask. Dep. Miner. Resour., Rep. 54, 33p.

____ (1966): The geology of the Pelican Narrows and Birch Portage Narrows areas, Saskatchewan; Sask. Dep. Miner. Resour., Rep. 93, 68p.

Sibbald, T.LI. (1972): 63-M-3-E: Sandy Narrows (east half); in Summary Report of Geological Investigations Conducted in the Precambrian of Saskatchewan; Sask. Dep. Miner. Resour_, p4-10.

Thomas, D.J. (1988a): Bedrock geological mapping, Pait Lake area (part of NTS 63M-3 and -4 and 63L-13 and -14 ); in Summary of Investigations 1988, Saskatchewan Geologi­cal Survey, Sask. Energy Mines, Misc. Rep. 88-4, p20-25.

____ (1988b): Bedrock Geology, Palf Lake area (part of NTS 63M-3, -4 and 63L-13, -14), Sheet 1: North; '. :20 000 scale prelim. map with Summary of Investiga­tions 1988, Saskatchewan Geological Survey, Sask. En­ergy Mines, Misc. Rep. 88-4.

____ (1986c): Bedrock geology, Palf Lake area (part of NTS 63M-3, -4 and 63L-13, -14), Sheet 2: South; 1:20 000 scale prelim. map with Summary of Investigations 1988, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 88-4.

Trzcienski, W.A. Jr., Rodgers, J., and Guidotti, C.V. (1992): Al­ternative hypotheses lorthe Chain Lakes "Massif", Maine and Quebec; Amer. J. Sci., v292, p508-532.

Summary of Investigations 1993