Revision Bedrock Geological Mapping, Neagle Lake-Errington Lake Area (Parts of NTS 63L-9 and -16) 1

B.A. Reilly

Reilly, B.A. (1992): Revision bedrock geological mapping, Neagle Lake-Errington Lake area (parts of NTS 63L-9 and -16); in Summary of Investigations 1992, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 92-4.

During the 1992 field season approximately 225 km2

were mapped in detail (1 :20 000 scale) in the Neagle Lake-Errington Lake Area. Mapping included the area south of Matheson and Welsh lakes, north of Wolf Lake, east of Williams Creek, and west of the West Channel, Amisk Lake.

A major objective is to better understand the controls on base metal and gold deposits in the region. Emphasis is being placed upon the application of physical volcanol­ogy and lithogeochemistry in refining the volcanic stratig­raphy, mapping, and geochemical study of intrusive rocks, as well as detailed structural analysis of the com­plex fault/shear systems transecting the region. Relative ages for volcanism, plutonism, metamorphism, and deformation events based on field relationships are being tested by high precision geochronological methods.

Revision bedrock geological mapping in the Neagle Lake- Errington Lake area is a component of the Sas­katchewan Geological Survey's multi-disciplinary, multi­year Project Seagull and includes revision bedrock geological mapping by Reilly (1990, 1991) and col­leagues D. Thomas (1989, 1990, 1991, this volume), B. Slimmon (1991, this volume), and K. Ashton (1990). Project Seagull is part of a larger Canada-Manitoba-Sas­katchewan Shield Margin NATMAP Project focused a!ong the Precambrian Shield-Paleozoic margin.

1. Previous Work

Tyrrell (1902), Mcinnes (1909), and Bruce (1916, 1918) recorded the first reconnaissance geological surveys in the Flin Flon-Amisk Lake region. These surveys were followed by detailed studies by Wright and Stockwell (1934), Pearson (1951 ), Byers and Dahlstrom ( 1954), Fox (1976a, b), Ayres et al. (1981). Walker and Watters (1982), and Pearson (1983).

2. General Geology The area around Neagle Lake and Errington Lake lies in the Flin Flon greenstone belt2 of the Flin Flon-Snow Lake Domain, the most southern exposure of the Trans­Hudson Orogen (Lewry and Collerson, 1990; Hoffman, 1990). Supracrustal rocks in the map area have been

ascribed to the Amisk Group, which is dated at 1886 ±2 Ma (Syme et al., 1987). The stratigraphic sequence appears to consist of older mafic volcanics overlain by intermediate volcanics with subordinate felsic volcanics (Figure 1 ). Sedimentary rocks in the north are believed to be volcanogenic. Major intrusions include the pre- to syn-tectonic Oddan Lake Pluton and the post-tectonic Neagle Lake Pluton which has been dated at 1837 ±5 Ma (Ansdell and Kyser, 1991) and 1946 + 14/-6 Ma (Ashton et al., 1992). Minor intrusions include syn-vol­canic bodies of gabbro/diorite and rare quartz feldspar porphyry. Post-tectonic dykes of mafic and felsic com­position are found locally.

Regional metamorphic grade increases towards the northwest. Contact metamorphism may be associated with emplacement of the Neagle Lake Pluton. Retrograde metamorphism is associated with late structures.

Early east-west-trending D1 folds are deformed by north­south-trending D2 folds to produce a complex fold inter­ference pattern. The dominant regional fabric found throughout the area is a north-south-trending axial planar foliation associated with the D2 deformation. Diapiric emplacement of the Neagle Lake Pluton has su­perimposed on this regional fabric a contact strain aureole, D3. Brittle-ductile shear zones developed during D4 deformation are concentrated along the east­ern margin of the area and are inferred to be associated with the main West Channel Fault. Faults and topographic lineaments which transect the area are inter­preted as a product of late stage brittle 05 deformation.

Several mineralized showings are found in the map area. Base metal occurrences, including the Fon Zone and the Abbott Lake Showing, are hosted by felsic vol­canics. Gold occurrences, such as the Wing Showing and the Bud Showing, are structurally controlled and as­sociated with D4 brittle-ductile shear zones.

3. Lithological Units

a) Mafic Volcanic Rocks

Mafic volcanics are exposed as a continuous unit along the western margin of the area (from Abbott Lake to

(1) Saskalchewan Project A 112 1s funded jn 1992-93 under the Canada-Saskatchewan Partnership Agreement on Mineral Development 1990·95. (2) All of the Precambrian rocks in the map area have been metamorphosed and the prefix mela will be omitled when referring o these rocks.

16 Summary of Investigations 1992

+ + + + + + + +

+ + + + + LEGEND + + + + + + + + + + +

+ + + + =Neu gl e + + + + L u k e P lu ton

+ + + + + + + ~ Grcrn,t e + + + L uke Plu t on

+ + ,-------,, +

~ Odd on ,-------,, + L o k e Pl uton ~-~ ,-------,,

I -,------,, I Dio r i t e / G0bbr o ,-------,, .

~ Se dih e n t s

PJ F el si c - : nt er Vo lcan ic: s

~ Mo.f ie V olcanics

------ F l f o ld

-------- Sheer Zo ne

0 2 3

1 12 5,000

Figure 1 - Geological sketch map of the Neagle Lake-Errington Lake area. A, Matheson Lake; B, Wildfong Lake; C, Welsh Lake; D, Abbott Lake; E, Neagle Lake; F, Errington Lake; G, Oddan Lake; H, West Channel, Amisk Lake; I, Wolf Lake; ELA, Errington Lake Anricline; OLS, Oddan Lake Syncline; WLA, Wolf Lake Anticline; MBS, Muskeg Bay Synform.

Wolf Lake) and in the centre of the area (north of Er­rington Lake). These rocks crop out in the core of the Er­rington Lake Anticline and the Wolf Lake Fold (Anticline) to the south (Ashton, 1990). Minor units of mafic vol­canics are locally interbedded with intermediate vol­canics.

Flow rocks are the dominant rock type and are typically massive; however, pillow flows are common. Minor flow units, exhibiting pillow breccia, plagioclase phenocrysts, mafic phenocrysts, and quartz amygdales, are also

Saskatchewan Geological Survey

present. Mafic pyroclastic rocks, including tuff breccia, lapilli tuff, and bedded tuff, are less common than flow rocks and are generally intercalated with intermediate volcanic rocks.

The mafic volcanic rocks are tholeiitic basalts which show juvenile island arc affinities as determined by Fox (1976a). Fox also recognized an upward trend in the stratigraphy from basal olivine normative basalts to quartz-normative basalts. Watters and Ashton (1991)

17

documented a possible transitional to back-arc environ· ment for mafic volcanic rocks to the south.

b) Intermediate Volcanic Rocks

Intermediate volcanic rocks, which are most abundant in the Neagle Lake-Errington Lake area, were subdivided in the field into andesites and dacites based on colour index. Massive to plagioclase porphyritic units are dominant amongst the andesitic flows. In well-exposed sections on the west shore of Amisk Lake, individual flows can be distinguished by the presence of flow top and bottom breccia. Flow breccias and quartz amyg­daloidal flows, best exposed on the south shore of Er­rington Lake, are also common. Pillow and pillow brec­cia units are a minor component. Pyroclastic varieties, which include tuff breccia, lapilli tuff, and ash and crystal tuft, are generally well sorted and massive to well bedded. Fragments are both monolithic and heterolithic and matrix-supported. Grain size gradation is observed in some of the well-bedded units. A unit of poorly-sorted heterolithic tuff breccia, well exposed on Errington and Amisk Jakes, is interpreted as a debris flow.

The dacites, which are Jess voluminous than the an­desites and predominantly pyroclastic, have similar char­acteristics to the pyroclastic andesitic units. Lapilli, ash, and crystal tuft units are most common, but tuff breccia units also occur.

Geochemical studies by Fox (1976a) and Walker and Watters (1982) identified these intermediate volcanic rocks as a classical well differentiated calc-alkaline se­quence distinct from the underlying tholeiitic basalts in the area and from the tholeiitic basalts from the East Amisk area (Parslow and Gaskarth, 1988) and Flin Flan area (Watters, 1990, 1991).

c) Felsic Volcanic Rocks

Except around Abbott Lake and northwest of Neagle Lake, felsic volcanics are rare. They are typically inter­bedded with the intermediate volcanic rocks and are generally pyroclastic. Tuff breccia, lapilli, ash and crystal luffs are common. Fe!sic volcanic rocks which crop out northwest of Neagle Lake are intercalated with elastic sediments, some of which are thought to have been derived from felsic volcanics (Schwann, this volume). A tuff breccia, of uncertain origin, composed of felsic frag­ments in a mafic matrix, is well exposed on the south shore peninsula of Errington Lake. The felsic volcanic rocks form part of the calc-alkaline sequence identified by Fox (l976a) and Walker and Watters (1982). Felsic rocks occur in many places adjacent to brittle-ductile shear zones and faults. It is not dear whether these rocks are rhyolites or silicified intermediate (or even mafic) volcanic rocks.

d) Sedimentary Rocks

Epiclastic sedimentary rocks crop out between Mathe­son Lake and Welsh Lake in the north and at the mouth of Neagle Creek at Amisk Lake; the latter can be corre­lated with the northern exposures. Minor layers of sedi­ments are also intercalated elsewhere with the volcanic

18

rocks. Greywackes are the dominant rock type; minor layers of argillite and thin beds of shale and arkose are also recognized. The greywackes range from massive to very thinly bedded. Quartz stringers are common in the northern exposures. In the north, where metamor­phic grade is higher, the sediments are psammopelitic.

e) Major Intrusions

The Oddan Lake Pluton, which crops out between Er­rington Lake and Wolf Lake, comprises mainly medium­to coarse-grained biotite granodiorite and hornblende granodiorite. Quartz diorite and tonalite are found along its southern margin. Contacts between the components of the intrusion are gradational. As the intrusion is folded and possesses the regional fabric of the sur­rounding supracrustal rocks, it is interpreted as pre- to syn-tectonic.

The oval-shaped Neagle Lake Pluton, which crops out between Neagle Lake and Welsh Lake, is a coarse­grained body which is typically plagioclase porphyritic and ranges in composition from quartz monzonite to diorite. The core of the intrusion consists of diorite which is mantled by quartz diorite. Granodiorite is con­centrated along the north and east margins of the in· trusion. Quartz monzonite and tonalite occurs locally. In­ternal contacts are gradationaJ. Small dykes of peg­matite, aplite, gabbro, diorite, lamprophyre, and am­phibolite intrude the main intrusion and are also found as apophyses in adjacent country rock. As the pluton is discordant and deforms the regional fabric along its mar­gins, it is interpreted as post-tectonic. Small satellite in­trusions in the MacDonald Lake area are similar to the Neagle Lake Pluton with which they are believed to be related.

f) Minor Intrusions

Small bodies of medium-grained gabbro to diorite com­position are the most common minor intrusions in the area. They crop out in the Errington Lake area, mainly amongst the mafic volcanic rocks. The bodies are con­cordant, but irregularly-shaped discordant bodies occur in some places. Metamorphic assemblages and struc­tural fabrics observed in these intrusions are similar to those found in the surrounding mafic volcanic rocks, in­dicating a pre- to syn-tectonic origin. A distinctive coarse­grained gabbro, which is locally plagioclase porphyritic and brecciated along the margin, crops out on the southeast shore of Errington Lake. Pre- to syn-tectonic felsic intrusions are rare. A concordant medium- to coarse-grained quartz diorite to granodiorite quartz­feldspar porphyry is located east of Oddan Lake.

Weakly to strongly discordant post-tectonic dykes of mafic and felsic composition occur locally in the supracrustal sequence. The dykes average l to 2 m in width and contacts are sharp, irregular, and typically ex­hibit chilled margins. The dykes are generally fine to medium grained and include massive and plagioclase porphyritic varieties.

Summary of Investigations 1992

4. Metamorphism Metamorphic grade increases from the southeast towards the northwest of the area. At least three metamorphic facies are provisionally recognized as fol­lows:

1. Upper greenschist facies is found in the southeast (West Channel, Amisk Lake-Lady Jane Lake area). Volcanics of mafic and intermediate composition are dominated by chlorite ± biotite ± actinolite ± epidote.

2. Metamorphic grade increases to lower amphibolite facies in the centre of the area (Errington Lake­Neagle Lake area); mafic and intermediate volcanic rocks are predominantly composed of hornblende ± biotite ± garnet. Felsic volcanics and sediments contain biotite ± garnet ± staurolite.

3. The sediments in the north of the area are at middle amphibolite facies, containing biotite ± garnet ± sillimanite (Schwann, this volume and Ashton, 1992).

The northward increase in grade is interpreted as due to a regional metamorphic event which was probably in­itiated during 01 folding and peaked during 02 folding. Ashton (1990, 1992) describes a similar north­northwestward increase in metamorphic grade in the west Amisk Lake area.

Contact metamorphism associated with emplacement of the Neagle Lake Pluton was first proposed by Byers and Dahlstrom (1954), who described andalusite por­phyroblasts along the east and north margin of the in­trusion. Andalusite was not found, however, on the northern margin of the intrusion in the Welsh Lake area during this study. De Tombe (1988) interpreted the presence of andalusite on the eastern margin of the in­trusion as part of the regional metamorphic as­semblage. On the other hand, coarse garnet por­phyroblasts and local staurolite porphyroblasts found this summer along margins of the Neagle Lake Pluton are provisionally interpreted as a contact aureole.

Retrograde metamorphic assemblages of lower greenschist facies associated with 04 brittle-ductile shear zones and composed of calcite ± sericite ± chlorite ± epidote represent a post-peak metamorphic event. Mafic and intermediate rocks have been retrogressed to chlorite schists and other chlorite-rich as­semblages, and felsic rocks have produced sericite schists and other sericite-rich assemblages. Carbonate generally occurs in all assemblages.

5. Structural Geology

The area is deformed by two fold systems, one with axes trending east-west and the other with approximate­ly north-south axes. These have been labelled D 1 and 02 respectively.

The east-west 01 fold set is exemplified in the Er­rington Lake Anticline, which was first recognized by

Saskatchewan Geological SuNey

Fox (1976a) on the basis of geochemical stratigraphy. The steeply-dipping axial plane of this structure lies within the mafic volcanic rocks. Stacking of mafic vol­canic pillow flows indicate that the north limb of this structure youngs to the north. Graded bedding and flame structures found in the intermediate volcanics on the south limb of the fold, although complicated by sharp reversals due to soft sediment deformation, indi­cate stratigraphic tops to the south.

Two other 01 folds have been mapped: the Odden Lake Syncline lying south of the Errington Lake An­ticline and the Wolf Lake Fold (Anticline), which ex­tends to the south (Ashton, 1990). No axial planar fabric has been recognized in association with the 01 folding. On the other hand, a moderately developed steeply-dip­ping north-south-trending regional penetrative foliation transects all rock units except the Neagle Lake Pluton. This is interpreted as an axial planar fabric associated with 02 north-south folding. The presence of north­south folding was first identified by Byers and Dahlstrom (1954) as the Muskeg Bay Syncline. Ashton (1990) renamed this structure the Muskeg Bay Synform. The fold interference pattern in the map area can be at­tributed to the extension of the Muskeg Bay Synform, which bisects the Oddan Lake Pluton and continues north through Errington Lake. The Muskeg Bay Synform is interpreted to plunge moderately to the north on the basis of 02 minor folds, and stretching and intersection lineations associated with the axial planar fabric.

Contact strain around the Neagle Lake Pluton and its satellites has been labelled as the 03 deformation. The aureole of contact strain, believed to be associated with the emplacement of the plutons, is about 100 m wide and entirely envelopes the intrusions. Evidence for con­tact strain includes the development of a strong planar and stretching linear fabrics along the margin of the in­trusions and adjacent country rocks, and folding of the 02 planar fabric. Generally, the linear fabric is more strongly developed than the planar fabric within the aureole, locally producing steeply plunging L-tectonites. Coaxial minor fold axes are found in the intrusions, but are better developed in the country rocks. The style of folding changes from tight isoclinal folds to open-gentle folds with increasing distance from the intrusive con­tacts. A weakly developed foliation found within the in­trusions may be related to a magmatic origin. The con­tact strain aureole mantling the Neagle Lake Pluton and its satellites is interpreted as indicating forceful emplace­ment characteristic of a diapir.

Along the west side of Amisk Lake, southwards from the Neagle Lake Pluton, are a series of north-northwest­trending brittle-ductile shear zones. These zones are typically less than 10 m wide, and rarely as much as 100 m, and increase in number and size closer to the West Channel of Amisk Lake. They are interpreted as splays of the much larger West Channel Fault mapped by Byers and Dahlstrom (1954).

Shearing in these zones is manifest as a strong to in­tense planar fabric locally accentuated by millimetre­scale tectono-metamorphic layering, boudinaged and sheared quartz and carbonate veins, and transposed

19

layering. Early rootless isoclinal folds and sheath folds occur locally. These are folded by more common asym· metric shear folds. Z-folds are dominant over S-folds. These folds plunge shallowly to the northwest and are coaxial with the stretching lineation observed in the shear zones. A steeply dipping north-northwest-trending axial planar foliation is locally developed. The kinematics of these zones are not clearly understood at this time.

Byers and Dahlstrom's (1954) mapping suggests that the West Channer Fault is truncated by the Neagle Lake Pluton and Ashton et al. (1992) suggest that the fault might displace the pluton. The relationship of the brittle· ductile shear zones to the West Channel Fault and the Neagle Lake Pluton has yet to be determined. As the shear zones crosscut the regional fabric and apparently displace the Neagle Lake Pluton, they are tentatively in­terpreted as 04 deformation structures. Retrograde metamorphic assemblages, which are associated with the brittle-ductile shear zones, indicate that shearing post-dated the peak of regional metamorphism.

Late stage faulting, DS, is interpreted from strong topographic lineaments of low relief which transect the area and from mapped lithological offsets. These form a regional northeast and northwest conjugate set. Where observed on the ground, some of these structures show evidence of ductile shearing. Others, however, show no associated pervasive fabric and are interpreted as brittle faults. The faults are interpreted as steeply dipping.

6. Economic Geology Mining companies have actively explored for base me­tals and gold in the Flin Flon-Amisk Lake region area since the early part of the century. The following descrip­tions of showings in the map area are compiled from off­confidential data in the Saskatchewan Energy and Mines Mineral Assessment Files, the Saskatchewan Mineral Deposits Index, and reports by Byers and Dahlstrom (1954), Beck (1959) and Coombe (1984, 1991 ).

a) Gold

Summary of Showings

The Bud Showing is located on the West Side of Amisk Lake (approximately 1.75 km east of Oddan Lake). The showing was staked in 1954 and development work con­sisted of a small trench and two short drill holes. The host rock is a felsic intrusion which intrudes intermediate volcanic rocks. Mineralization is controlled by a one metre-wide northerly trending fracture zone. Pyrite and chalcopyrite are found within quartz veins and wall rock. The drill holes failed to intersect the mineralized zone. The gold content of the zone is unknown.

The Wing Showing (Assessment File 63L-9-0052) is lo­cated approximately 2.5 km north of Oddan Lake on the northeast shore of a small unnamed lake. The showing was staked by Wing Wong in 1949 and development work consisted of four small trenches. The ground was

20

restaked as the Rex claims in 1953 and in 1954-57 Noranda Mines Limited conducted geophysics and drilled three holes. The host rocks are intermediate-felsic volcanics. Mineralization is controlled by a 60 to 90 cm north-northwest-trending shear zone. Pyrite and chal­copyrite are found disseminated in the partly chloritized structure. The gold content of the zone is unknown.

Mineral Potential

Iron sulphides, including pyrite and chalcopyrite, and gossanous zones were identified in the area within zones of brittle-ductile shear which are interpreted as 04 splays of the West Channel Fault. Extensive veins of quartz ± carbonate and local tourmaline are commonly associated with these mineralized zones. The zones are typically altered and include carbonatization, silicifica­tion, chloritization, and sericitization.

Gold occurrences in the West Amisk area are spatially associated with the West Channel Fault. Gold is found in gold-quartz veins which lie in or near the boundaries of shear zones and in sulphide-rich shear zones (Pear­son, 1983). The association of gold occurrences and brittle-ductile shear zones supports a model for struc­turally controlled gold mineralization.

b) Base Metals

Summary of Showings

The Fon Zone (Assessment Files 63L-16-0043, -0053) is located approximately 1.5 km west-northwest of Neagle Lake (approximately midway between Neagle Lake and Matheson Lake). The showing was first discovered in 1968 by Hudson Bay Exploration and Development Company by follow-up drilling of a wide, west-northwest­trending electromagnetic anomaly. Since 1968, more than 45 holes (totalling 7816 m) were drilled. A series of five massive sulphide lenses were delineated for an es· timated 5, 126,000 tons of 4.6 percent zinc. Copper, lead, silver, and gold are also present. The host rocks are predominantly felsic volcanics with minor interca­lated intermediate and mafic volcanic rocks (Schwann, this volume). The lenses occur within a zone of altera­tion approximately 1100 m Jong and 100 m wide that ex­tends from surface to a depth of more than 600 m. The mineralized lenses dip steeply to the north and in­dividual lenses range from 100 to 250 m in length and are typically less than 5 m wide. Pyrrhotite, pyrite, sphalerite, chalcopyrite, and minor galena occur as dis· seminations or in massive form in the lenses. Alteration is dominated by carbonatization, Fe-Mg metasomatism, aluminous alteration, and silicification (Schwann, this volume).

The Abbott Lake Showing (Assessment Files 63L-16· 0042, -0044, -0051, 0056, and -0223) is located at the northwest end of a small unnamed lake approximately 1 km east of the north end of Abbott Lake. Hudson Bay Exploration and Development Company Limited iden­tified several conductors from ground electromagnetic surveys in the Neagle-Matheson lakes area in 1968. Be­tween 1969-74 more than thirty holes (totalling 4250 m)

Summary of Investigations 1992

were drilled on a northwest-trending conductor at the site of the showing. Copper, zinc, silver, and gold were found. The host rocks are northwesterly-trending felsic volcanics and volcaniclastics which are variably altered to chlorite schist and sericite-biotite-staurolite schist. Pyrite, chalcopyrite, sphalerite, and rare galena are found disseminated to semi-massive.

Mineral Potential

Several occurrences of iron sulphides are found in the map area in the felsic volcanic rocks, and less common­ly in the intermediate and mafic volcanic rocks. Dissemi­nated pyrite ± chalcopyrite ± pyrrhotite ± sphalerite generally comprise 2 to 3 percent of the host rocks. Gos­sanous zones are locally associated with the sulphide occurrences.

The predominantly calc-alkallne island arc volcanic se­quence in the West Amisk area contrasts with tholeiitic MORB volcanic sequence of the East Amisk area and the tholeiitic island arc volcanic sequence in the Flin Flon area which host Cypress- and Kuroko-type vol­canogenic massive sulphide deposits, respectively. These differences led Fox (1976a) to suggest that poten­tial massive sulphide deposjts in the West Amisk area are likely to have a somewhat different stratigraphic style as compared with those in the East Amisk and Flin Flon area and may be richer in lead.

7. Acknowledgments

Senior assistant Roberta Hicks and junior assistants Dwayne Morrison, Thomas Schuster, and Darren Ander­son provided competent and cheerful assistance. Field visits by Bob Macdonald, Bill S!immon, and Larry Heaman proved helpful. An early version of this manuscript was critically reviewed by Ken Ashton and Bob Macdonald.

8. References Ashton, K.E. (1990): Geology of the Snake Rapids area, Flin

Fion Domain (parts of NTS 63L-9 and -10); in Summary of Investigations 1990, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 90-4, p4-12.

{1992): Geology of the Mari Lake area, Sas­~~k-a~tc~h-e-wan; Geol. Surv. Can., Open File Rep. 2444, map

at 1 :50 ODO scale.

Ashton, K.E., Hunl, P.A., and Froese, E. (1992): Age con­straints on the evolution of the Flin Flon volcanic belt and the Kisseynew gneiss belt, Saskatchewan and Manitoba; in Radiogenic Age and Isotopic Studies, Rep. 5, Geol. Surv. Can., Pap. 91-2, p55-69.

Ansdell, K.M. and Kyser, K.T. (1991 ): Plutonism, deformation and metamorphism in the Proterozoic Flin Flon greenstone belt, Canada: Limits on timing provided by the single-zircon Pb-evaporation technique; Geol., v19, p518-521.

Ayres, L.D., Van Wagoner, N., and Van Wagoner, S. (1981): Physical volcanology of the Amisk Lake Volcano; in Sum­mary of Investigations 1981, Saskatchewan Geological Survey, Sask. Miner. Resour., Misc. Rep. 81-4, p47-51.

Saskatchewan Geological Survey

Beck, L.S. (1959): Mineral occurrences in the Precambrian of northern Saskatchewan (excluding radioactive minerals); Sask. Dep. Miner. Resour., Rep. 36, 134p.

Bruce, E.L. (1916): Amisk-Athapapuskow Lake area; Geol. Surv. Can., Sum. Rep. 1915, p126-130.

~~~~ (1918): Amisk-Athapapuskow Lake district; Geel. Surv. Can., Mem. 105, 91p.

Byers, AR. and Dahlstrom, C.D.A. (1954): Geology and mineral deposits of the Amisk-Wildnest lakes area, 63L-9, 63L-16, Saskatchewan; Sask. Dep. Miner. Resour., Rep. 14, 177p.

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

--~~ (1991): Base Metals in Saskatchewan; Sask. Ener­gy Mines, Open File Rep. 91-1, 218p.

de Tambe, J. (1988): The metamorphic stability fields of the Welsh Lake Area in east-central Saskatchewan; unpubl. B.Sc. thesis, Queen's Univ., 46p.

Fox, J.S. (1976a): Some comments on the volcanic stratig­raphy and economic potential of the West Amisk Lake area, Saskatchewan; Sask. Res. Council, Circ. 9, 30p.

(1976b): Volcanic stratigraphy and mineralization - ~i~n~lh~e- A~misk Group; Geol. Assoc. Can./Min. Assoc. Can.,

Jt. Annu. Meet., Edmonton, Alberta, Prog. Abstr., v1, p72.

Hoffman, P.F. (1990): Subdivision of 1he Churchill Province and extent of the Trans-Hudson Orogen; in Lewry, J.F. and Stauffer, M.R. (eds.), The Early Proterozoic Trans-Hud­son Orogen of North America, Gaol. Assoc. Can, Spec. Pap. 37, p15-39.

Lewry, J.F. and Collerson, K.D. (1990): The Trans-Hudson Oro9en: Extent, subdivision, and problems; in Lewry, J.F. and Stauffer, M.R. (eds.), The Early Proterozoic Trans-Hud­son Orogen of North America, Geol. Assoc. Can, Spec. Pap. 37, p1-14.

Mcinnes, W. (1909): Explorations on the Churchill River and South Indian Lake; Geol. Surv. Can., Summ. Rep., 1908, p87-92.

Parslow, G.R. and Gaskarth, J.W. (1988): Proterozoic rocks of east-central Saskalchewan: Geochemistry, structure, and mineralization controls; in Summary of Investigations 1988, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 88-4, p127-139.

Pearson, W.J. (1951): The origin and history of the Neagle Lake pluton in the Amisk Lake area; unpubl. M.A. thesis, Univ. of Sask., 72p.

Pearson, J.G. (1983): Gold rnetallogenic studies: Flin Flon­Amisk Lake area; in Summary of Investigations 1983, Sas­katchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 83-4, p67-74.

Reilly, B.A. (1990): Bedrock geological mapping, Mystic Lake-West Arm, Schist Lake area (part of NTS 63K-12); in Summary of Investigations 1990, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 90-4, p25-35.

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-~~~ (1991): Revision bedrock geological mapping, Mystic Lake-Kaminis Lake area (parts of NTS 63K-12 and 63L-9); in Summary of Investigations 1991, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 91-4, p9-15.

Slimmon, W.L. {1991): Revision bedrock geological mapping, Table Lake area (part of NTS 63L-9); in Summary of Inves­tigations 1991, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 91-4, p16-20.

Syme, E.C., Bailes, A.H., Gordon, T.M., and Hunt, P.A. (1987): U-Pb zircon geochronology in the Flin Flan belt: Age of Amisk volcanism; in Manit. Energy and Mines, Report of Reid Activities 1987, plOS-107.

Thomas, D.J. (1989): Geology of the Douglas Lake-Phantom Lake area (part of NTS 63K-12 and -13); in Summary of In­vestigations 1989, Saskatchewan Geological Survey, Sask. Energy Mines. Misc. Rep. 89-4, p44-54.

--~- (1990): New perspectives of the Amisk Group and regional metallogeny, Douglas Lake-Phantom Lake area; in Summary of Investigations 1990, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 90-4, p13-20.

-~-~ (1991): Revision bedrock geological mapping, Bootleg Lake-Birch Lake area (part of NTS 63K-12 and 63L-9); in Summary of Investigations 1991, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 91-4, p2-8.

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Tyrrell, J.B. (1902): Explorations in the northeastern portion of the district of Saskatchewan and adjacent parts of the Dis­trict of Keewatin; Geol. Surv. Can., Ann. Rep., va, 1900, Rep. F, 48p.

Walker, D. and Watters, B.R. (1982): Geochemistry of metavol­canic rocks, Amisk Lake west area; in Summary of Inves­tigations 1982, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 82-4, p24-30.

Watters, B.R. (1990): Lithogeochemical studies in the Flin Flon-Amisk Lake area; in Summary of Investigations 1990, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 90-4, p44-47.

____ (1991): Lithogeochemical studies, east Amisk Lake area; in Summary of Investigations 1991, Sas­katchewan Geological Survey., Sask. Energy Mines, Misc. Rep. 91-4, p21-27.

Watters, B.R. and Ashton, K.E. (1991): Geochemistry and tec­tonic setting of metabasaltic rocks from the Snake Rapids area, Flin Flon Domain; in Summary of Investigations 1991, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 91-4, p130-134.

Wright J.F. and Stockwell C.H. (1934): West half of Amisk Lake area, Saskatchewan; Geol. Surv. Can., Annu. Rep., 1933, pt. c .. p12-22.

Summary of Investigations 1992