50

Project 8502

Kisseynew Metallotect Geochemical Study by G.R. Parslow1 and J.W. Gaskarth2

Parslow, G.R. and Gaskarth, J.W. (1985): Kisseynew metallotect geochemical study; in Summary of Investigations 1985, Saskatchewan Geological Survey; Saskatchewan Energy and Mines, Miscellaneous Report 85-4.

This project follows on four others which have investigated the geochemistry of the Amisk-type volcanics and associated rocks in the southeastern part of the Saskatchewan Shield, namely the East Amisk, Annabel Lake, Hamell Lake, and Hanson Lake projects (Parslow and Gaskarth, 1981 , 1982a, 1982b, 1983, 1984, in prep.). Some of these studies delineated a major shear zone separating Amisk-type rocks from Kisseynew-type rocks along the line of Johnson Lake, Annabel Lake and Annabel Creek. This zone extends into Manitoba to the north of Embury Lake (Trout Lake Mine), through Tartan Lake and is probably represented at Puffy Lake by the mylonite zone of Zwanzig (1984). The studies have also shown that the rocks in the East Amisk area have ocean floor affinities, very different from those with arc-type affinities to the north (Flin Flon) and west (Hanson Lake). The recent copper-nickel discovery at Namew Lake lies due south and along the trend of these rocks.

There has been much discussion about the possibility that the Kisseynew rocks are the more highly metamorphosed lateral equivalents of the Amisk and Missi sequences (review by Moore, 1977; Bailes, 1980). A geochemical study of the numerous basic units in the Kisseynew rocks might throw some light on the possible equivalence to the Amisk volcanics.

In Manitoba, Robertson (1953) divided the Kisseynew into the Nokomis Group and the Sherridon Group, mainly on structural evidence. Gale (1981) refined the classification. Zwanzig (1984) correlated the Nokomis temporally with Amisk-type rocks, and the Sherridon with Missi. He also postulated a major unconformity at the base of the Sherridon. Gale and Ostry (1984) described a thin unit of variable volcanic and sedimentary rocks lying at the top of the Nokomis group directly beneath the Sherridon, and designated this unit the Kisseynew Metallotect because it contains massive sulphide deposits (e.g., Sherridon) and gold occurrences (e.g., Puffy and Nokomis Lakes).

The overall objectives of the present study are 1) to test the concept of the presence of a stratigraphically controlled metalliferous horizon, or horizons. within the Kisseynew Domain in Saskatchewan adjacent to the Manitoba border, and if such a horizon appears to exist, 2) to initiate a lithostratigraphic and lithogeochemical description and interpretation of the unit(s).

'Department of Geology, University of Regina. 2Qepartment of Geological Sciences. University of Aston. Birmingham. U.K. Project contracted to the University of Regina with funds provided under the Saskatchewan component of the Canada­Saskatchewan Subsidiary Agreement on Mineral Development 1984-89.

The initial methodology is to:

1) geologically map selected parts of the suspected metalliferous horizon(s) (i.e., the 'Kisseynew Metallotect') in Saskatchewan at appropriate detailed scales using geological parameters outlined by the Manitoba Geological Services Branch, and by any other appropriate indicators;

2) collect rock samples for geochemical study on selected traverses across the 'stratigraphy' of the metallotect;

3) undertake any necessary petrographic studies of the samples;

4) undertake whole rock, trace element and precious metal analyses of the samples;

5) use the data to establish, or otherwise, any possible stratigraphic controls for massive sulphide and/ or gold occurrences within the metallotect;

6) use the data to establish exploration guidelines and target areas within the metallotect.

The above studies were intended to interface with a concurrent 1 :20,000 scale regional geological mapping project in the same general area, but unfortunately, this project was abandoned due to unforeseen circumstances. With no regional mapping as back-up, the geochemical project was modified to concentrate more on the amphibolitic horizons of the presumed metallotect over a larger area, rather than detailed mapping of geological sections in limited areas. Consequently, step (1) above has not been covered in quite as much detail as was originally intended.

Much of the area under discussion has been mapped previously, as 15-minute quadrangles on a 1 :63,360 scale. by Byers and Dahlstrom (1954), Cheesman (1956), Johnson (1966), Macdonald (1975) and Pyke (1961, 1965). A study of these maps shows that there are belts of hornblende gneiss. calc-silicate rocks and amphibolites that may represent 'metallotect horizon(s)' within the Kisseynew of Saskatchewan. Whether or not these belts separate the Nokomis and Sherridon subunits as they apparently do in Manitoba, and whether or not there is a major unconformity between the subunits as reported by Zwanzig (1984), is not apparent from the maps or from the work carried out this summer. K. Ashton's detailed work in the area (this volume). presently being done under contract to the Geological Survey of Canada. should clarify the identification of Nokomis- and Sherridon-type rocks in Saskatchewan.

51

Figure 1 • Loe 1· a ,on of study areas.

The accompanying map of east-central Saskatchewan, is divided into five blocks. The southeastern block represents the main area of this study; within this block five areas and one traverse (Fig. 1) were studied in some detail (Figs. 2 to 6 show sample locations on a larger scale; the traverse is indicated as (6) on Fig. 1 ). Figure 1 also shows the location of 'metallotect-type' rocks with a stippled decoration. On the large-scale maps (Figs. 2 to 6) these rocks are denoted by an arrowhead pointing to the sample location. The northeastern block was not surveyed except for one small area on the south side of Kipahigan Lake (see location (7) on Fig. 1). Apparent 'metallotect-type' horizons. marked with a stipple, are more disrupted and less continuous than in the area to the south. The northwestern block was not visited; here the existing geological map (Johnson, 1966) shows no indication of any amphibolitic or basic gneisses or volcanic rocks which may be interpreted as 'metallotect'. The western area was also not visited; however, mapping by Pyke (1961) indicates the presence of a considerable number of units which are probably 'metallotect-type' rocks repeated by folding.

Eastern Mari Lake: Area 1

52

This area comprises a northwest trending and easterly dipping sequence of mixed supracrustal and mafic rocks abutting the western margin of a large. strongly foliated granodiorite body. Contained within the mafic rocks is the Dolly gold showing (Coombe, 1984).

The most distinctive rock type observed in the vicinity of the gold showing is a porphyritic basaltic rock (six or more metres thick) containing up to 40 percent subhedral plagioclase phenocrysts (up to 25 mm long) with some glomeroporphyritic clusters and partial flow alignment. We interpret this rock as a basaltic flow unit which has been preserved virtually undeformed. This unit thins considerably to the north and exhibits intense shearing on its western margin. to the extent that the original rock type is virtually unrecognizable. The eastern margin is unexposed and its southerly extension terminated by the east bay of Mari Lake. Close to the western contact are quartz-rich ultramylonitized rocks with 'quartz eyes· which are probably the flattened vestiges of disrupted quartz veins or pseudotachylites(?). Within the basalt there is a 300 mm 'layer' of heavily sheared fine-grained felsic rock, which is either a stratigraphic unit within the basalt or of tectonic origin. As noted above, this package of 'metallotect-type' rocks is bounded to the east by granodiorite while to the west of the sheared contact is a series of hornblende and biotite gneisses containing both foliated granitic layers and later unfoliated granitic material.

To the south, across the east bay of Mari Lake and along strike from the Dolly showing, a zone of mafic rocks was identified by Macdonald (1975). A traverse along this unit (Fig. 2) identified the presence of hornblende gneisses grading to amphibolite in places. At one locality, a coarse­grained plagioclase/hornblende rock and a coarse-

gabbroic and/or ultrabasic rocks. At the extreme south end of the traverse some calc-silicate horizons crop out in close association with the more typical 'metallotect-type' rocks. Evidence of shearing is commonplace throughout this generally mafic unit.

Figure 2 - Sample locations, eastern Mari Lake ( Area 1 ).

grained honrblende/garneVlight brown biotite (phlogopite?) rock occur together with some sulphides (mainly pyrrhotite). These rocks are interpreted as relict gabbroic and/or ultrabasic rocks. At the extreme south end of the traverse some calc-silicate horizons crop out in close association with the more typical 'metallotect-type' rocks. Evidence of shearing is commonplace throughout this generally mafic unit.

The northern continuation of the 'metallotect-type' rocks is terminated, possibly by shearing out, about 1 km north of the Dolly showing. However, a series of traverses further north clearly identified a zone of hornblende gneisses and a few units of amphibolite. trending in the same direction and to the northwest of the showing. At two localities the rocks are very similar to but more deformed than the porphyritic basalt. Since many of these more northerly outcrops (some of which have been trenched) are pyritic, rusty weathering and contain rare chalcopyrite. we consider that this sequence of rocks represents the continuation of the Dolly showing rock package (i.e .. the 'metallotect') north of the shear. The sulphide mineralization is confined to the eastern margin of this northern package.

The only other 'metallotect-type' rocks observed in Area 1 were encountered on two traverses about 1.5 km west of the packages described above, consisting of thin units of hornblende gneiss and amphibolitic gneiss with some pyrite and chalcopyrite.

Central Mari Lake: Area 2 In Area 2, 'metallotect-type' rocks are found only to the

53

' tN tN ·: ..

' .. ...

· .. ·~ •,

•,

J u····.·. . . . . . .

I

J ..

. '-....

•.

' ' ....... "·· '•

~ .....

' ...

""' 1 km 0 1 km

Figure 3 - Sample locations, central Man Lake ( Area 2). Figure 4 - Sample locations, northern Mari Lake ( Area 3).

east of the northernmost narrows of Mari Lake (Fig. 3). These rocks lie in two zones, a thin westerly unit and a thicker eastern unit, and appear to be the northern continuation of the units recognized in Area 1. The dominant rock type is hornblende gneiss with sporadic amphibolite units. Garnets are common but irregularly distributed and in places give the rocks a 'knobbly' appearance on weathered surfaces. Traces of sulphides are present in some outcrops. Thin calc-silicate interlayers occur in the sequence. The extreme northern portion of the eastern 'metallotect-type' unit is considerably thinned.

Northern Mari Lake: Area 3 In Area 3 the two 'metallotect-type' horizons are believed to continue northwards along the eastern side of the lake (Fig. 4). However. a third horizon is found on islands in the centre of the lake. The two easterly horizons consist of hornblende gneisses, amphibolites and thin calc-

0

' ' ' . \

0

if .. 1 km

Figure 5 - Sample locations, Melgurd Lake (Area 4).

54

silicate interlayers as described above, but no well­preserved igneous fabrics were observed. At one locality, on the eastern edge of the larger of the two horizons, chalcopyrite and associated malachite staining were found.

The third horizon consists essentially of medium- to coarse-grained amphibolite, with up to 5 percent bronze mica (possibly phlogopite), which varies from massive in the south to a less homogeneous and more gneissic rock in the north. The coarser rock in the southern section is tentatively identified as a gabbro with sheared margins.

The following inferences can be drawn from the Mari Lake traverses:

1) 'Metallotect-type' rocks occur in the Kisseynew rocks of eastern Saskatchewan and correlate with those described in Manitoba.

~

lJ q

' 0 • 1 k m '·. · ":to a t

Figure 6 - Sample locations, Roberts Bay, Wildnest Lake ( Area 5 ).

2) The metallotect package is very varied, ranging from gabbros and basalts, through amphibolites and calc­silicates, to hornblende gneisses. Although deformation has destroyed most igneous fabrics, enough palimpsest features are recognizable to identify the package as igneous, containing both extrusive and intrusive rocks.

3) Although the Manitoba metallotect is shown as a single unit or zone, the present work identifies at least three units. Whether these units are indeed stratigraphically discrete or are structural repetitions of a single unit is not clear in the Mari Lake area.

4) As in Manitoba, gold and base metals are associated with the package.

Having identified previously mapped amphibolites and/or hornblende gneisses in the Mari Lake as 'metallotect-type' horizons, it was decided to examine some other areas that, according to existing geological maps, contain similar rock types. The two main areas selected were Melgurd Lake (Area 4) and Roberts Bay on Wildnest Lake (Area 5). Limited investigations were also done on little Mari Lake (Location 6), the west side of Wildnest Lake and the northwest part of Kipahigan Lake (Location 7).

Melgurd Lake: Area 4 The southeastern and western sides of Melgurd Lake are occupied by large patches of mafic rock mapped by Cheesman (1956, Unit 5) as amphibolite and (to the west) calc-silicate gneiss. Traverses this summer (Fig. 5) showed that these rocks form an interlayered sequence, in places containing pyrite and/or chalcopyrite. The similarities between this package and those observed at Mari Lake leads us to believe that these rocks also represent a 'metallotect-type' horizon. The presence of considerable carbonate-bearing material in association with amphibolites and hornblende gneisses does not detract from the concept of the 'metallotect' being largely volcanogenic in origin.

On the eastern side of the lake, an extensive area of coarse-grained basic rock, in some places containing specks of chalcopyrite, was observed. This rock is poorly foliated and consists largely of amphibole and feldspar with variable quantities of either biotite or garnet. Primary igneous textures, such as large feldspar phenocrysts (up to 30 percent of the rock), are present in places. We consider that these rocks represent a large gabbroic intrusion. Observed contacts are strongly sheared and the original 'gabbroic' texture has been destroyed, the result being a banded hornblende gneiss. A brief visit to a small lake about 4 km south indicated the presence of virtually identical gabbroic rocks. It is considered likely that the Melgurd lake gabbroic body extends at least some 6 km. Moreover. airphoto and previous mapping information lead us to postulate that this unit extends a further 10 km to the southeast. The elongate shape of this gabbroic

55

body is typical of previously described 'metallotect' horizons.

Roberts Bay: Area 5 This area was visited to investigate the northeast-trending zones of amphibolites. hornblende gneisses and calc­silicates mapped by Cheesman (1956). The rocks encountered constitute two zones (Fig. 6), the easternmost of which comprises interlayered amphibolitic and calc-silicate rocks very similar to those present on the west side of Melgurd Lake. The other zone is largely composed of calc-silicate rocks. The conclusion is reached that these rocks also form one or more 'metallotect' horizons.

Brief visits further to the west on Wildnest Lake also encountered calc-silicates and amphibolites which probably also represent other possible 'metallotect' horizons.

Although relict igneous fabrics are uncommon, the overall impression is that these rocks in the western part of the main area of study are volcanogenic.

Little Mari Lake: Location 6 A traverse across the hornblende gneiss unit of Byers and Dahlstrom (1954) at the south end of Little Mari Lake encountered units of amphibolite and calc-silicate, and one thick (10 m) hornblendite layer within the hornblende gneisses. The sequence is very similar to others described above and thus the hornblende gneisses are interpreted as probable ' metallotect' horizons.

Kipahlgan Lake: Location 7 A study of some localities of the diopside - calc-silicate granulite and hornblende gneisses of Pyke (1965) in the northwestern part of Kipahigan Lake was undertaken to see if they had any characteristics typical of 'metallotect' horizons further south.

It was observed that the area is of much higher grade (Rees, 1980) and the incipient melting and breakdown of rock units is much in evidence. However, some exposures do exhibit remnants of basic rocks containing sulphides, such as hornblendites. that have survived the pervasive granitization common throughout the area. It is concluded that 'rnetallotect-type' horizons exist here (as outlined in Fig. 1) but that their lateral continuity has been disrupted.

The Kisseynew Metallotect - An Interpretation As a result of the 1985 field work and a study of the available literature, the following points are considered important in the development of any evolutionary model for the region:

1) 'Metallotect-type' rocks are variable and occur in thin belts, but all are readily explained as being volcanogenic.

2) The multiplicity of 'metallotecHype' units is apparent in all areas investigated.

3) Kisseynew-type rocks, including 'metallotect-type· horizons, are terminated in the south by a major east­west shear zone.

4) Amisk-type rocks lie to the south of the east-west shear zom:.

5) Rocks south of the shear zone are generally of upper greenschist facies, while to the north the grade increases abruptly across the shear and reaches hornblende granulite facies just northwest of Kipahigan Lake (the northernmost part of the present study area) .

6) Foliations throughout the Kisseynew rocks in the area studied have shallow dips (values less than 20° are common). Pearson (1972) suggested that nappe­like folds are present in the Wildnest-Tyrrell Lakes area. and Macdonald (1975) identified recumbent isoclinal and nappe-style folding in the Mari Lake area.

7) Outcrop patterns of 'metallotect-type' rocks on published maps, around Wildnest and Attitti Lakes, look like refolded isoclinal folds (F •). Such extensive isoclinal folding has not been documented in either the Amisk-type rocks or in the La Ronge volcanic belt.

8) The Flin Flon and Lynn Lake volcanic belts are separated by the bilaterally symmetrical gneisses of the Kisseynew Domain and its central granitoid complex (MacRitchie quoted by Moore. 1977). This domain thus appears to be anticlinorial.

9) Late Archean to early Proterozoic dates have been obtained from the Sahli Gneiss dome in the Hanson Lake block (Bell and Macdonald, 1982; Van Schmus et al., 1985) and also in the McMillan Point granite nearby (Bickford and Van Schmus, this volume). Kisseynew-type gneisses occur beneath Amisk-type volcanic rocks in the Jackpine Lake anticline just south of the above dated basement (Gaskarth, 1967, 1971).

10) A recent review of available Rb-Sr data for the la Ronge and Fl in Flon Domains (Watters and Armstrong, 1985) documents some metasedimentary rock isochron points plotting above the 1900 Ma crustal growth curve which may be the result of an older basement component in these rocks.

11) Kisseynew-type gneisses east of the La Ronge

56

volcanic belt have constant facing directions to the west (Sibbald, pers. comm., 1985).

12) The east side of the La Ronge volcanic belt is terminated by a major shear zone (Lewry, pers. comm., 1985).

It is proposed that the above observations can be explained most simply by having the Kisseynew stratigraphically beneath the Amisk and at a much deeper level in the crust at the onset of the Hudsonian Orogeny. A significant thermal event caused a major uplift of the Kisseynew, with concomitant nappe emplacement. resulting in the observed gross bilateral symmetry of the Kisseynew Domain. The higher level rocks above the thermal uplift would not be deformed in the same style, would be disrupted, and would be preserved only at the margins of the high-grade nappe complex and separated from it by major shear zones.

The major implications of this model are:

1) The Flin Flon - Snow Lake and La Ronge - Lynn Lake volcanic belts are the disrupted fragments of the products of a single volcanic event. This simplifies any plate tectonic model in that only one destructive plate margin is required rather than two contemporaneous ones.

2) The multiplicity of metallotect horizons can readily be explained by repetition, a consequence of the F, nappe event.

3) Considerable lateral translat ion of Kisseynew-type rocks has occurred, and the contact zones between the volcanics and the high grade gneisses have great tectonic significance.

Economic Implications The above model has several important implications for the mineral potential of the region:

1) Mineralization within the metallotect horizons does not correlate with mineralization in the lower grade volcanic sequences (e.g., Amisk-type volcanic rocks).

2) Shear zones separating the high-grade gneisses from the lower grade volcanics have great potential for gold mineralization. We note. tentatively, that the east-west shear zone through Annabel Lake might extend across the Tabbernor Zone into the Wapawekka Lake area (cf. Macdonald and Broughton. 1980).

3) The geochemistry of the lower grade volcanic rocks indicates that there are both arc- and ocean floor-type environments. Thus, at least two types of massive sulphide deposit can be expected (e.g., Flin Flon-type vs. Namew Lake-type).

4) Significant gold occurrences, which are found in all three of the above environments, appear to be structurally controlled and, although some are apparently stratabound, they are probably epigenetic.

5) The Attitti Lake and Scimitar Lake complexes (Macdonald, 1981). which contain many apparent metallotect horizons possibly due to nappe-generated repetitions of a single unit or units, are deserving of more attention.

Acknowledgements We wish to acknowledge the help of L. Schick, D. Riley and M. Kolebaba for the high standard of their field assistance. We are also indebted to J. Pearson (Resident Geologist, Creighton) and J. Siryj for their help and hospitality.

References Bailes, A.H. (1980): Geology of the File Lake area: Manit.

Dep. Energy Mines. Miner. Resour. Div., Geol. Rep. 78-1, 134p.

Bell, K. and Macdonald, R. {1982): Geochronological calibration of the Precambrian Shield in Saskatchewan; in Summary ot Investigations 1982, Sask. Geol. Surv., Misc. Rep. 82-4, p17-22.

Byers. A.A. and Dahlstrom, C.D.A. (1954): Geology and mineral deposits of the Amisk - Wildnest Lakes area, Saskatchewan; Sask. Dep. Miner. Resour., Rep. 14, 177p.

Cheesman. R.L. (1956): The geology of the Mari Lake area. northeastern Saskatchewan: Sask. Oep. Miner. Resour., Rep. 23. 40p.

Coombe, W. (1984): Gold in Saskatchewan; Sask. Geol. Surv., Open File Rep. 84-1, 134p.

Gale. G.H. (1981) : Mineral deposit studies in the Flin Flon area; in Report of Field Activities 1981 . Manit. Oep. Energy Mines. p45-55.

Gale, G.H. and Ostry, G. (1984): GS-18: Stratabound gold mineralization in the Kisseynew gneiss terrain; in Report of Field Activities 1984, Manit. Dep. Energy Mines, p73-80.

Gaskarth, J.W. (1967): Petrogenesis of Precambrian rocks in the Hanson Lake area. east-central Saskatchewan: unpubl. Ph.D. thesis, Univ. Sask.

_____ (1971 ): Petrogenesis of Precambrian rocks in the Hanson Lake area, east-central Saskatchewan; Can. J. Earth Sci .• v8, p820-843.

Johnson, R.L. (1966): The geology of the Nemei Lake

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area (west half). Saskatchewan; Sask. Dep. Miner. Resour., Rep. 107, 23p.

Macdonald, R. (1975): Semi-reconnaissance in three areas, Pelican Narrows (63M); in Summary of Investigations 1975, Sask. Geol. Surv. , p35-43.

____ (1981) : Compilation bedrock geology: Pelican Narrows and Amisk Lake Areas: in Summary of Investigations 1981 , Sask. Geol. Surv., Misc. Rep. 81 -4, p16-23.

Moore, J.M.Jr. (1977): Orogenic volcanism in the Proterozoic of Canada; Geol. Assoc. Can .• Spec. Pap. 16, p1 27-148.

Parslow, G.R. and Gaskarth. J.W. (1981): Flin Flon base metals project: Annabel Lake area; in Summary of Investigations 1981 . Sask. Geol. Surv .. Rep. 81 -4, p101 -104.

_ _ ___ (1982a): Hanson Lake geochemical project: in Summary of Investigations 1982. Sask. Geol. Surv .. Misc. Rep. 82-4, p23.

_ _ _ __ (1982b): Flin Flon base metals project: Hamel! Lake area; in Summary of Investigations 1982, Sask. Geol. Surv., Misc. Rep. 82-4, p73-75.

_____ (1983): Geochemical studies in the Flin Flon and Hanson Lake areas: in Summary of Investigations 1983. Sask. Geol. Surv .. Misc. Rep. 83-4, p80-82.

____ (1984): Geochemistry of the East Amisk area: Sask. Energy Mines, Open File Rep. 84-23. 156p.

_ _ _ _ _ (1985a): Geochemistry of the Hanson Lake area: Sask. Energy Mines, Open File Rep. (in press).

____ (1985b): Geochemistry of the Annabel Lake area; Sask. Energy Mines. Open File Rep. (in prep.).

_ _ ___ (1985c): Geochemistry of the Hamel! Lake area: Sask. Energy Mines, Open File Rep. (in prep.).

Pearson. O.E. (1972) : The location and structure of the Precambrian Kisseynew Gneiss domain of northern Saskatchewan; Can. J. Earth Sci., v9, p1235-1249.

Pyke, M.W. (1961 ): T he geology of the Attitti Lake area (west half), Saskatchewan; Sask. Dep. Miner. Resour .. Rep. 54, 33p.

_ _ ___ (1 965): The geology of the Nemei Lake area (east half), Saskatchewan; Sask. Dep. Miner. Resour .. Rep. 97, 39p.

Rees. C .J. (1980): Metamorphism in the Canadian Shield of northern Saskatchewan; unpublished M.Sc.

thesis, Univ. Regina; Sask. Miner. Resour., Open File Rep. 82-2, 136p.

Robertson, D.S. (1953): Batty Lake map-area, Manitoba; Geol. Surv. Can., Mem. 271 , 55p.

Van Schmus, W.R. and Bickford, M.E. (1984): Preliminary U-Pb data for the trans-Hudson orogen in northern Saskatchewan; in Summary of Investigations 1984, Sask. Geol. Surv., Rep. 84-4, p81-85.

Van Schmus. W.R., Bickford, M.E.. Lewry, J.F. and Macdonald, R. (1985): U-Pb geochronology of the

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T rans-Hudson Orogen in northern Saskatchewan, Canada (abstr.); for presentation at International Conference on Proterozoic Fold Belts, Daiwin, Australia, August 1985.

Watters, B.R. and Armstrong, R.L. (1985): Rb-Sr study of metavolcanic rocks from the La Range and Flin Flon domains, northern Saskatchewan; Can. J. Earth Sci., v22, p452-463.

Zwanzig, H.V. (1984): GS-12 Kisseynew Project: Lobstick Narrows - Cleunion Lake, Puffy Lake and Nokomis Lake areas; in Report of Field Activities 1984; Manit. Dep. Energy Mines, p38-45.