bedrock geology of the northern janice lake and burbidge lake … · 2019. 1. 8. · the...

Saskatchewan Geological Survey 1 Summary of Investigations 2013, Volume 2

Bedrock Geology of the Northern Janice Lake and Burbidge Lake Areas, Wollaston Domain (parts of NTS 74A/14 and /15)

J. Fetter

Fetter, J. (2013): Bedrock geology of the northern Janice Lake and Burbidge Lake areas, Wollaston Domain (parts of NTS 74A/14 and 74A/15); in Summary of Investigations 2013, Volume 2, Saskatchewan Geological Survey, Sask. Ministry of the Economy, Saskatchewan Geological Survey, Misc. Rep. 2013-4.2, Paper A-5, 18p.

This report is accompanied by the map separate(s) entitled: Fetter, J. (2013): Bedrock geology of the northern Janice Lake area, Wollaston Domain (parts of NTS 74A/15); 1:20 000-scale preliminary geology map with Summary of Investigations 2013, Volume 2, Saskatchewan Geological Survey, Sask. Ministry of the Economy, Misc. Rep. 2013-4.2-(2.1). __________ (2013): Bedrock geology of the Burbidge Lake area, Wollaston Domain (parts of NTS 74A/14 and /15); 1:20 000- scale preliminary geology map with Summary of Investigations 2013, Volume 2, Saskatchewan Geological Survey, Sask. Ministry of the Economy, Misc. Rep. 2013-4.2-(2.2).

Abstract The Janice-Burbidge lakes area, within the east-central Wollaston Domain, is underlain by a thick succession of northeast-trending, variably deformed and metamorphosed, arkose, calc-silicate–bearing siliciclastic rocks, fanglomerate, conglomerate, and wacke of the Rafuse Lake and Janice Lake formations. Higher metamorphic grade rocks on southwestern Burbidge Lake are composed of psammopelite and minor pelite of the Bole Bay Formation. A variety of granitoid to pegmatitic dykes have intruded the supracrustal rocks.

Five episodes of deformation and have affected the rocks. D1 resulted in the development of a foliation (S1) of variable intensity. S1 has mostly been transposed parallel to compositional layering, and therefore is believed to be a composite foliation. D2 formed tight to isoclinal F2 folds. D3, which produced the main structural style, is characterized by tight to isoclinal northeast-trending, doubly plunging F3 folds. A pervasive, steep, dominantly northwest-dipping axial planar S3 foliation commonly has transposed earlier S0/S1/S2 fabrics. D4 formed northwest-trending, upright folds, expressed as a weak crenulation on S3. D4 was relatively weak and had little effect on the regional structural trends. D5 produced widespread brittle faults, which mainly trend north to northwest and crosscut all of the earlier structures.

Two Hudsonian metamorphic events, M1 and M2, are distinguished based on textural relationships between the similar metamorphic minerals of different generations. M1 began before the peak of D1 deformation and ended during D2 deformation and M2 was broadly coeval with, and outlasted, D3 deformation. Lower amphibolite facies conditions within the arkoses of the Janice Lake and Rafuse Lake formations occurred during M1, as indicated by the presence of garnet, biotite, and hornblende. Partial melts are found locally, possibly associated with M2 suggesting middle to upper amphibolite facies. Metamorphic grade reached upper amphibolite facies northwest of Burbidge Lake as indicated by the stability of sillimanite, cordierite, and K-feldspar relative to the apparent lack of muscovite, within the pelitic rocks.

Detailed mapping in the summer of 2013 revealed that the prospective Janice Lake Formation extends for at least 15 km northeast of Janice Lake, where it has an apparent thickness of 2 km. The northeast-trending Burbidge Lake shear zone, which has also been traced 15 km northeast of Janice Lake, causes repetition of the Janice Lake Formation to the southwest. Extension of the Janice Lake Formation further to the north than previously appreciated highlights a prospective area for sediment-hosted Cu mineralization similar to that found in the Janice and Rafuse lakes areas.

Keywords: Wollaston Domain, Wollaston Supergroup, Paleoproterozoic, Janice Lake, Burbidge Lake, fanglomerate, sediment-hosted copper deposits, bedrock mapping.

1. Introduction The Janice Lake project was initiated to augment previous detailed mapping in the east-central Wollaston Domain by Delaney (1994 to 1995) and to evaluate the economic potential of areas along strike of known Cu occurrences (Figure 1). This project is being conducted in conjunction with a study of the surficial geology of the area (Hanson, this volume).

http://economy.gov.sk.ca/SOI2013V2_M2.1http://economy.gov.sk.ca/SOI2013V2_M2.2


Figure 1 – Regional 1:250 000-scale geological map of east-central Wollaston Domain showing locations of the two detailed map areas (A and B outlined in black). Inset map shows the region with respect to domainal subdivisions of the Canadian Shield in northern Saskatchewan. Informal lake names appear in single quotations.

Anderson LakeInlier

JohnsonLakeInlier

BurbidgeLake

JaniceLake

JunoLake

‘StolenBoot’Lake

‘RabbitBush’Lake

ThompsonRiver

KarinLakeInlier

FraserLakesInlier

Precambrian Domains

RafuseLake

Wollaston Domain

Wollaston SupergroupArkose/calcareous arkose

Fanglomerate/conglomerate

- - - UNCONFORMITY - - -

Slate, phyllite, mica schist

Pelitic gneiss

- - - UNCONFORMITY - - -

ArcheanFelsic orthogneiss

Mylonitic gneiss

Granite/granodiorite

250 km

Wol

lasto

n

10 km0

A

B


This work also builds on previous investigations that focussed on the stratigraphic setting (Coombe, 1994; Delaney, 1993, 1994; Delaney et al., 1995, 1996, 1997) and on its structural setting (Tran and Yeo, 1997; Tran et al., 1998: Yeo and Savage, 1999) within the Paleoproterozoic supracrustal rocks of the Wollaston Supergroup on the southeastern side of the central Wollaston Domain. This year’s mapping will be combined with Delaney’s (1994 to 1997) work to create a compilation map for the area extending from Burbidge to Nelson lakes.

In 2013, an 11-week mapping program was carried out in two areas; one encompassing the north end of Burbidge Lake and the other, a region to the northeast of Janice Lake from Juno Lake almost to the Thompson River (Figures 1 and 2). Much of the map area northeast of Janice Lake is covered by dense forest; last having been burned about 30 years ago. Where there is outcrop, it is commonly covered with thick lichens and/or moss. In contrast, a majority of the map area centered on Burbidge Lake was burned in 2010. The burn associated with that fire was very spotty, but it did result in some excellent lichen-free exposures.

2. Previous Work The first published reconnaissance work in the area was performed by McMurchy (1936) and Rice (1951) of the Geological Survey of Canada. In 1969, Rath completed an industry-supported M.Sc. thesis on the petrology and base metal mineralization in the Janice Lake area. Scott (1973) mapped the west half of the 74A/15 NTS map sheet, at a scale of 1:63,360 and made detailed geological maps of the Janice and Rafuse showings. The base metal potential in the George Hills, Johnson and Kaz lakes, and Geikie River areas was investigated by Coombe in 1977 (Coombe, 1991). Regional 1:250 000-scale compilation bedrock geology and metallogenic maps were prepared by Ray (1983) and Scott (1986), respectively. In 1984, a regional lake sediment and water geochemical survey was completed by the Geological Survey of Canada (Geological Survey of Canada,1984; Hornbrook and Friske, 1988).

A series of more detailed mapping projects and investigations of base metal potential continued from 1994 to 1997 (Delaney 1994; Delaney et al., 1995, 1996; Tran and Yeo, 1997). A publication summarizing all the known sediment-hosted base metal deposits of the Wollaston Domain was released by Coombe (1994).

3. Regional Geological Setting The Burbidge Lake–northern Janice Lake map area is in the east-central margin of the Wollaston Domain, which is bounded by the Needle Falls shear zone to the southeast and by the Wollaston-Mudjatik Transition Zone to the northwest. The domain consists of a tightly northeast-trending fold and thrust belt of Paleoproterozoic metasedimentary rocks containing inliers of Archean granitoid rocks exposed in structural domes. With respect to the map area, Archean basement rocks are exposed in the Johnson River inlier to the north, the Anderson Lake granite to the south, and the Fraser lakes inlier to the west (Figure 1; Ray, 1983). These inliers are composed of mostly leucocratic coarse-grained granite with lesser tonalitic felsic gneisses. The contact between the Archean inliers and Paleoproterozoic sedimentary rocks is marked by a sharp structurally modified unconformity.

The Paleoproterozoic metasedimentary rocks, referred to as the Wollaston Supergroup (Yeo and Delaney, 2007), record deposition of rift, passive margin, and foreland basin successions, which were deposited during the opening and closing of the Manikewan Ocean (Stauffer, 1984). The Burbidge-Janice lakes area is underlain by rocks stratigraphically situated within the upper sequence of the Wollaston Supergroup, at the base of the Geikie River Group (Table 1). The Wollaston Domain was intruded by a variety of granitoid rocks (Harper et al., 2005).

4. Unit Descriptions Table 1 provides a summary of previous authors’ subdivisions of the rock units within the immediate mapping area. The stratigraphic nomenclature used by Delaney et al. (1995) and Yeo and Delaney (2007) was adopted for this study.

a) Daly Lake Group The oldest rocks in the Wollaston Supergroup exposed in the study area belong the Daly Lake Group. The Daly Lake Group comprises pelite, psammopelite, psammite, and quartzite, showing an overall upward increase in compositional maturity (Yeo and Delaney, 2007). Exposure of the Daly Lake Group is shown through its member, the Bole Bay Formation, which rests structurally above the younger Geikie River Group due to thrusting northwest of Burbidge Lake.


Figure 2 – Simplified geological maps of the: A) northern Janice Lake area and B) Burbidge Lake map areas. Informal lake names appear in single quotations.

Legend

Glacial Drift

Pegmatite

Protomylonite

Arkose and calc-silicate

Arkose and quartz areniteArkoseArkose and wacke

Conglomerate

Calc-silicate brecciaFelsic rockWackeSiltstone and wackeGranitized siltstone

Quartz arenite and wackeArkose

Polymictic conglomerate

Conglomerate and sandstone

Fanglomerate

Pelite to psammopelite

Psammite to psammopelite

Undivided Intrusive Rocks

--- Intrusive Contact---Paleoproterozoic

Wollaston SupergroupFraser Lakes Formation

Undivided Supracrustals Rocks

Rafuse Lake Formation

Janice Lake Formation

--- Fault Contact ---

Bole Bay Formation

Symbols

Photo lineament

Thrust fault

Trace of F3 axial plane

Northern Janice Lake area (North Sheet)

Burbidge Lake area (South Sheet)

‘RabbitBush’Lake

‘StolenBoot’Lake

Burbidge Lake

0 21 km

0 21 km

N

N

Burbidge Lakeshear zone

Burbidge Lakeshear zone

Burbidge Lake shear zone

West Burbidge thrust fault

A

B

... ...


Table 1 – Comparison of stratigraphic nomenclature used in the study area by previous workers. Unit numbers correspond to their respective maps.

Bole Bay Formation

The type area of the Bole Bay Formation is about 50 km southwest of Janice Lake where it has a mapped true thickness of 120 m (Tran et al., 1998). At Burbidge Lake, the formation is characterized by a succession of cordierite- and sillimanite-bearing psammopelite and pelite (Figure 3).

Psammite to psammopelite (BBrn) is pink to pinkish grey weathering and medium grained, with local K-feldspar–rich partial melt layers. Selective hematization and minor sillimanite nodules are present. A strong foliation is developed (Figure 3A). The psammite is generally thickly bedded with mafic mineral content of less than 5%. In more psammopelitic to pelitic layers, K-feldspar–rich leucosome lenses containing cordierite and sillimanite, with biotite selvages comprise up to 10% of the rock. This unit is only found on the west side of Burbidge Lake. The contacts within the unit and with BBnp are transitional.

Pelite to psammopelite (BBnp) is grey to pink, fine to medium grained with distinct pinkish brown-grey irregular bodies of coarse-grained quartzofeldspathic leucosome (Figure 3B). The rocks are strongly foliated, locally containing coarse-grained white plagioclase porphyroblasts up to 4 cm in diameter and sillimanite nodules up to 5 cm in length (Figure 3C). The leucosome composes up to 60% of the rock and contains coarse-grained cordierite

Rock Unit This Study

Yeo and Delaney (2007)

Tran (2001)

Tran and Yeo

(1997)Delaney et al. (1995)

Delaney (1994)

Scott (1973)

Marble Hidden Bay Assemblage 28 16/17 15

Arkose and interbedded calc-

silicaterc Fraser Lakes Formation 26/27 15 rc rc 14

Arkose with intercalated

quartz areniterq rq

Arkose and interbedded

wacker2/r3 r2/r3 r2/r1 9

Arkose, psammite,

conglomerate, calc-silicate, and

calc-silicate breccias


Rafuse Lake Formation 13*

Rafuse Lake

Formationrp/cbx/ra/rqv

Fanglomerate and conglomerate with arkose and

minor pelite


Janice Lake Formation 23/24/25 12

Janice Lake Formation o/p1 11

Quartzite and arkose

Burbidge Lake Formation 21/22 13 6/7

Heterogeneous psammopelite to

psammite

Roper Bay Formation 20 11

Psammopelite to psammite

Thompson Bay Formation 19 10

Cordierite–sillimanite–

K-feldspar pelite to psammopelite

np/rn Bole Bay Formation 15 8/9 np 16

Gei

kie

Riv

er G

roup

Dal

y La

ke G

roup

* noted that it was a younger sequence but could not distinguish it form the Burgidge Lake Formation.


Figure 3 – Rocks of the Bole Bay Formation, Burbidge Lake. A) Interlayered psammite and psammopelite (unit BBrn) with tight northeast-trending F3 minor fold (station JF13-38-001: UTM 495201 m E, 6298960 m N); B) pelite and psammopelite (unit BBnp); over 50% of the outcrop is K-feldspar–rich leucosome containing cordierite and sillimanite (station JF13-34-001: UTM 495383 m E, 6298369 m N); C) sillimanite nodules flattened and aligned parallel to S1 (station JF13-38-003: UTM 495623 m E, 6298878 m N); and D) coarse-grained cordierite within leucosome (station JF13-38-003: UTM 495623 m E, 6298878 m N). Note: All UTM coordinates are in NAD 83, zone 13V.

(Figure 3D). Up to 2 to 3% magnetite is found locally. This unit underlies the northwestern side of Burbidge Lake and just east of ‘Rabbit Bush Lake’ 1 just outside the map margins.

b) Geikie River Group The term ‘Geikie River Group’ was proposed by Yeo and Delaney (2007) for the succession of conglomerate, arkose, calc-silicate–bearing arkose, calc-silicate rock, and marble unconformably overlying the Daly Lake Group. The majority of the two map areas are underlain by the Geikie River Group. Contacts between formations within the Group are typically transitional. Deposition of the Geikie River Group has been constrained to 1.88 to 1.86 Ga (Tran, 2001).


The Janice Lake Formation, the basal unit in the Geikie River Group, includes fanglomerate and conglomerate with interbedded arkose (Delaney et al., 1995). It is host to copper occurrences in the vicinity of Janice Lake. The Janice Lake Formation is found intermittently in the Wollaston Domain including, from north to south, the following areas: Duddridge Lake (Delaney, 1993), Haultain River (Tran et al., 1999), Highrock Lake (Yeo and Savage, 1999), Hills Lake (Delaney et al., 1997), and northeast of Wollaston Lake (Harper et al., 2005).

1 Informal lake names first appear in single quotations; subsequently the quotes are dropped.

A B

C D


Fanglomerate (JLo) is distinctively weathered to a mottled maroon colour. It is comprised of a poorly sorted framework of sub-angular to sub-rounded hematitic clasts, ranging from a few centimetres to meters in diameter, in a fine- to medium-grained quartzofeldspathic matrix (Figure 4A). At some places, clasts are no longer distinguishable due to alteration, granoblastic recrystallization of clasts and matrix, and/or deformation. The most abundant clasts consist of pebble to boulder-sized, maroon to buff, hematitic, laminated to massive arkose. Pebble-sized, sub-rounded, granitic, calc-silicate, amphibolite(?) and quartz clasts are rare. The ‘exotic’ nature of the granitoid and amphibolite clasts, and their smaller (2 to 6 cm in diameter) and better rounded character, suggest a more distal source than the arkosic clasts. In some outcrops the granitoid and quartz clasts have a weak internal fabric that is locally sub-parallel to the main foliation, but often oblique, possibly suggesting they were derived from a previously deformed terrain.

The fanglomerate has a whitish to grey, fine- to medium-grained quartzofeldspathic matrix containing up to 10% biotite. Locally, the epidote and biotite content combined can exceed 15% along with up to 10% calcite. The relative abundance of clasts to matrix ranges from less than 20% up to 80%. Tran and Yeo (1997) suggested the matrix farther south on Burbidge Lake is possibly a pseudomatrix, comprising largely recrystallized arkosic clasts ‘lost’ in the matrix.

The fanglomerate has been affected by a number of secondary processes that include late diagenetic alteration, metamorphic recrystallization, and syn- to post-tectonic development of partial melt segregations (Delaney et al., 1995). In some areas, these secondary processes have rendered the clasts unrecognizable. Therefore, most of the

Figure 4 – Fanglomerate of the Janice Lake Formation. A) Laminated and homogenous boulder-sized arkose clasts (station JF13-13-013: UTM 506129 m E, 6310337 m N); B) possible bedding contact (dashed line) distinguished by a change in clast size across middle of photograph (station JF13-13-013: UTM 506129 m E, 6310337 m N); C) flattened arkose clasts aligned parallel to regional S3 foliation with laminated arkose clasts perpendicular to it (station JF13-25-009: UTM 508498 m E, 6308803 m N); and D) strongly foliated fanglomerate (station JF13-30-006: UTM 510450 m E, 6311002 m N).

A B

C D


Figure 5 – Quartz-pebble conglomerate of the Rafuse Lake Formation, Burbidge Lake (station JF13-39-005: UTM 497515 m E, 6298445 m N).

fanglomerate appears to be matrix supported. Partial melting appears to have been selectively concentrated along clast boundaries and along crude bedding planes.

On an outcrop scale, the fanglomerate appears to exhibit crude beds of variable, metre-scale thickness depicted by the size and abundance of the arkose clasts (Figure 4B). Crude clast-supported beds of variable thickness with sorted, sub-rounded clasts ranging from 2 to 4 cm in diameter are interbedded with layers that contain angular to sub-angular, meter-sized clasts. These bedding contacts are generally sharp.

The fanglomerate is variably deformed (Figure 4C). In places, clasts are moderately to strongly elongated, and elsewhere there is a weak to locally very strong foliation defined by the degree of flattening of the clasts (Figure 4D). Many of the observed outcrops exhibited a high degree of deformation with only selective areas containing a weak to moderate foliation and lineation.

The fanglomerate unit is extensive throughout both the map areas (Figure 2). The contact between the fanglomerate of the Janice Lake Formation and the overlying Rafuse Lake Formation is sharp northwest of the Burbidge Lake shear zone (Delaney et al., 1995), whereas to the southeast, the fanglomerate is intercalated with siltstone and sandstone of the Rafuse Lake Formation in a narrow transitional zone.

Conglomerate and sandstone (JLro) is a sandstone-dominated succession of fine-grained, laminated rocks, locally characterized by hematite- and epidote-rich beds (JLro2). Clast-supported conglomerate beds less than 1 m thick were only found at one outcrop and are characterized by hematized arkose pebbles set within a fine-grained, quartzofeldspathic matrix. Very high magnetic susceptibility readings of 15 to 30*10-3 SI distinguish a mappable subunit, JLrom, which otherwise displays similar properties to JLro. This subunit was observed east of ‘Stolen Boot Lake’ (Figure 2).

Polymictic conglomerate (JLo2) is characterized by a light to medium grey, quartzofeldspathic matrix containing rounded to sub-rounded pebbles and cobbles of arkose, wacke, granitoid and vein quartz. Possible sandstone beds 1 to 2 m wide were observed at one locality within the unit just north of Burbidge Lake. The polymictic conglomerate is believed to be a facies equivalent of the fanglomerate.

Magnetite-bearing polymictic conglomerate (JLom) is distinguished from the other two conglomerate units on the basis of its anomalous magnetic susceptibility readings of 15 to 40*10-3 SI. The conglomerate has a similar clast composition and size range as JLo2 and appears to be matrix supported. The matrix typically contains between 5 to 10% mafic minerals dominated by biotite and hornblende.


The Rafuse Lake Formation is a heterogeneous succession of arkose, wacke, conglomerate, and calc-silicate breccia (Delaney et al., 1995), and hosts several copper occurrences in the Janice Lake area. The contact between the Rafuse Lake and Janice Lake formations is sharp. Relative stratigraphic positions within the Rafuse Lake Formation are uncertain.

Conglomerate (RLo) is a light grey to buff weathered unit locally with maroon mottling. It is characterized by an intact to disrupted framework of sub-rounded to rounded, pebble to cobble-sized, commonly elliptical clasts of quartzite and minor arkose (Figure 5). A minimum apparent thickness of about 50 m is implied at one location although most of the unit cannot be defined at the present scale of mapping. The matrix, which appears to have recrystallized, is composed of plagioclase-quartz-biotite. Typically the long axes of the elliptical quartzite clasts are aligned parallel to the main foliation and define a strong lineation.

The arkose (RLa) unit comprises a pink-buff to grey-weathered, fine-grained, thin- to medium-bedded succession. Local partial melt lenses comprise medium- to coarse-grained quartz, magnetite, and hornblende within fine-grained plagioclase. The unit is moderately to well foliated. Rath and Morton (1969) reported staurolite in an arkose unit east of Juno Lake, which is believed to be correlative to this unit.


Quartz arenite and wacke (RLqw) is buff to grey weathered and fine to medium grained. A strong foliation is defined by aligned biotite and amphibole, which together comprise up to 20% of typical rocks. Local leucosome blebs and segregations of amphibole and quartz occur in many of the outcrops. This unit is found on at the north end of Burbidge Lake (Figure 2B).

Siltstone and wacke (RLsw) is light to dark greyish brown on weathered surfaces, very fine to fine grained, and strongly foliated. The unit varies from homogenous siltstone to interbedded wacke laminae to beds containing up to 20% biotite. Quartz blebs and stringers also occur locally, and epidote is common as coatings on fractures and in clots. North of Janice Lake (Figure 2A), wacke, which is the main rock type in this unit, contains 20 to 25% biotite throughout, whereas east of Burbidge Lake (Figure 2B), siltstone with less than 10% biotite is the main rock type. A light grey weathered, fine-grained, quartzofeldspathic siltstone (RLswg) occurs locally in this unit east of Burbidge Lake. It is primarily composed of quartz and feldspar with minor biotite and is variably assimilated by fine-grained leucocratic granitoid partial melt. This unit is believed to be the distal lateral facies equivalent of RLsw, found only on the west side of the Burbidge Lake shear zone.

Wacke (RLw) is grey to greenish grey weathered, fine to very fine grained, and massive to well foliated. It is composed of plagioclase, quartz, biotite (10 to 20%), and epidote (5 to 10%). Disseminated magnetite is common; hornblende and actinolite are minor constituents. Leucosomal pegmatite and granite are common as irregular bodies and dykes within the unit. This is a recessive unit with very few outcrops observed north of Janice Lake.

Calc-silicate breccia (RLcbx) is a mottled greenish to light grey–weathered unit that contains subangular to subrounded fragments of fine-grained plagioclasite in a fine- to medium-grained matrix of actinolite and plagioclase that locally contains disseminated and patchy concentrations of medium- to coarse-grained actinolite and diopside. This unit occurs as 10 to 20 m thick lenses throughout the Rafuse Lake Formation.

A narrow unit of pink- to buff-weathered, fine- to very fine grained felsic rock (RLfel) was observed in a small area north of Burbidge Lake. Typical rocks are homogenous, massive and featureless with a mafic content of less than 5%.

c) Supracrustal Rocks This theorized younger succession of arkose, wacke, and arenite in the western part of the Janice Lake area, has not been previously assigned to a specific formation (see discussion below).

Arkose and interbedded wacke (r2) is pink to grey weathered, fine grained, and is thin to medium bedded with hematitic laminae and minor 1 to 2 cm thick layers of brownish grey wacke. It locally contains rare clots and lenses of actinolite and plagioclase. The unit contains up to 10% mafic minerals, mostly biotite and amphiboles. Light green epidote locally coats late fractures. Millimetre- to centimetre-scale, white partial melts and calc-silicate pods are also locally found.

Arkose (r3) is buff to greyish pink weathering, medium to thick bedded, fine to very fine grained, and granoblastic. The mafic minerals include less than 5% biotite and minor hornblende. Parallel to sub-parallel quartz-feldspar-hornblende veins and clots 2 cm wide obliquely crosscut the S3 foliation in the arkose. This unit is believed to be a lateral equivalent of r2 (Delaney et al., 1995). It also appears similar to RLa; however, it occupies a higher stratigraphic position (see discussions below). It is distinguished from the unit RLqw by its lower mafic content and high (over 25%) K-feldspar content.

Arkose with intercalated quartz arenite (rq) is only found on the northwest side of Burbidge Lake in association with the West Burbidge Lake thrust. It weathers light grey to buff and, in some areas that are more arkose dominant, brown to grey. It is very fine to fine grained and thinly to thickly bedded. The unit is weakly to strongly foliated and moderately to strongly lineated.

Fraser Lakes Formation

The Fraser Lakes Formation is a succession of calc-silicate–bearing arkose with intercalated calc-silicate–rich beds (Figure 6). The type area for this formation is at Fraser Lakes, 8 km northwest of the map area, where it has an apparent thickness of about 850 m (Delaney et al., 1996).

Arkose with intercalated calc-silicate (FLrc) is a light grey to pinkish white to green, bedded to laminated sequence that also contains minor wacke. Calc-silicate–rich beds range from 8 to 10 cm thick on Burbidge Lake to meters thick east of Rabbit Bush Lake. Distinctive differential weathering and pitting is typical of the calc-


Figure 6 – Fraser Lakes Formation. A) Typical differential weathering of intercalated calc-silicate and arkose (station JF13-38-007: UTM 496298 m E, 6298813 m N) and B) calc-silicate–rich layer within the Fraser Lakes Formation, Burbidge Lake (station JF13-18-005: UTM 506400 m E, 6311330 m N).

silicate–rich layers, which are composed of fine- to medium-grained plagioclase and quartz (up to 30%), medium- to coarse-grained actinolite (10 to 15%), and up to 20% combined diopside, epidote, and calcite. Amphibole and pyroxene, associated with quartz, are commonly concentrated along late fractures as pods and blebs, orientated both randomly and parallel to the S3 foliation. The arkose component is laminated to thinly bedded and contains less than 5% biotite. The foliation is weak to well developed and the rocks along the northwest side of Burbidge Lake are strongly lineated. The contacts within this unit appear to be gradational. This unit also appears to interfinger with many of the units.

Younger Intrusive Rocks

Several generations of granitic pegmatites of slightly varying compositions are common throughout both map areas. The granitic pegmatite dykes include generations that are: folded by F3 folds, aligned parallel to S3, and are sub-parallel to parallel to late D5 brittle faults. Varieties of the granitic pegmatites include those that are: 1) actinolite bearing; 2) magnetite bearing with thorium and uranium enrichment; 3) plagioclase rich with only minor potassium feldspar; and 4) muscovite and tourmaline bearing. The magnetite thorium- and uranium-rich pegmatitic dykes are commonly less than a meter thick, and generally less than half a meter thick. The average concentrations of U, Th, and K were based on two-minute analyses using a hand-held gamma and neutron radiation spectrometer (Radiation Solutions GR-135). The results are only averages and multiple readings at the same locality slightly vary. Therefore, they should not be taken as substitutes for direct rock assays. The highest thorium count was 166.6 ppm (station JF13-21-005: UTM 509474 m E, 6315476 m N; 5.7 ppm U; total count=1200) from just northwest of Stolen Boot Lake; whereas the highest uranium count was 199.4 ppm (station JF13-26-004: UTM 511690 m E, 6313936 m N; 66.8 ppm Th; total count=3300) from northeast of Stolen Boot Lake.

5. Structural Geology Variable degrees of deformation have led to some difficulty in correlating structures and related deformational episodes between different areas within the Wollaston Domain (Table 2). Based on the present study, the rocks have been affected by four major deformational events and late brittle faulting, all of which are attributed to the ca. 1.84 to 1.77 Ga Trans-Hudson orogeny.

D1 was responsible for the development of a foliation (S1) of variable intensity. Compositional layering has mostly been transposed by S1 to produce the main regional S0/S1 composite foliation. It is most apparent within the interbedded sequences of arkose and wacke (mainly unit r2 and rq). This first deformation event has been identified throughout much of the Wollaston Domain, and was previously attributed to thermal reworking of the basement and the emplacement of gneiss domes to levels near the basement/cover contact (Lewry and Sibbald, 1980). In contrast, Tran and Yeo (1997) suggested that D1 may have been produced by tectonic transport and crustal imbrication, resulting in moderate crustal thickening.

D2 is represented by tight to isoclinal folding of the S0/S1 fabric. F2 folds are recumbent, reflecting subhorizontal shortening, and are thought to be related to northwest-southeast convergence due to collision of major tectonic

A B


Figure 7 – Equal-area stereonet plot of minor, doubly plunging, F3, folds within the Bole Bay Formation, northwest of Burbidge Lake (n=13).

Table 2 – Comparison of deformation events documented by previous workers.

blocks (Tran and Yeo, 1997). Evidence of D2 is only seen locally in the Wollaston Domain and is often combined with D1, however is it probably both intense and regional extensive but often overprinted by the D3 deformation (see discussion below).

D3, which produced the northeast-trending structural fabric typical of the Wollaston Domain, formed by tight to isoclinal, doubly plunging, southeast-vergent F3 folds, generally with steeply, northwest dipping axial planes. In the Janice Lake area, L3 fabrics are best defined by elongated sillimanite nodules (Figure 3C), and tight folds (F3) are best developed within the pelites and psammopelites of the Bole Bay Formation (Figure 7). The fold geometry varies from Class 2 to Class 3 (Ramsay, 1967), but is more commonly Class 2, with relatively thin fold limbs and thickened hinges.

Late D3 Reverse Faulting

The study area is cut by two main northeast-trending–,ductile-brittle, steeply to moderately northwest-dipping reverse faults: the West Burbidge Lake thrust fault and the Burbidge Lake shear zone.

The West Burbidge Lake thrust fault is a northeast-trending, ductile-brittle fault (Tran and Yeo, 1997) that runs through the western part of Burbidge Lake. Numerous outcrop-scale, brittle-ductile, reverse faults with extensive gently to moderately plunging tectonic stretching lineations are associated with this fault zone (Figure 8). The West Burbidge Lake thrust fault has thrust predominantly pelitic rocks of the older Bole Bay Formation over arkoses of the much younger undivided sedimentary succession that overlies the Rafuse Lake formation. On the basis of the difference in metamorphic grade between the Bole Bay Formation and the sedimentary units, the vertical displacement maybe up to several kilometres.

The Burbidge Lake shear zone is a northeast-trending, brittle-ductile fault zone (Delaney et al., 1995) that is marked by a linear topographic low running through the northeastern arm of Burbidge Lake, the eastern arms of Janice Lake, and to the northeast within the

Event Major Structural FeaturesThis

StudyTran

(2001)

Tran and Yeo (1997)

Delaney et al. (1995)

Delaney (1994)

Lewry and

Sibbald (1980)

Ray (1975)

Scott (1973)

D5 Brittle faults trending west-northwest D5 D5 D4 D5 D5

D4 Open upright northwest-trending folds and crenulations D4 D4 D3 D4 D4 D3

D3

Tight to isoclinal, northeast-trending doubly plunging folds (F3); regional pervasive steeply dipping axial planar folation (S3)

D3 D3 D2 D3 D3 D3 D2 D2

D2

Weak steeply dipping to subvertical axial planar foliation (S2) tight to isoclinal folding (F2)

D2 D2 D2

D1

Regional axial planar foliation transposed on S0, rare rootless isoclinal folds, tectonic transport and crustal imbrication

D1 D1 D1 D1 D1 D1

D1 D1


Figure 8 – Equal area stereonet plot of tectonic stretching lineations and the fault plane associated with the West Burbidge Lake thrust (n=11; mean trend=235°; mean plunge=28°).

Figure 9 – Equal area stereonet plot of tectonic stretching lineation and fault plane associated with the Burbidge Lake shear zone (n=19; mean trend=291°; mean plunge=67°; part of data set is taken from Delaney et al. (1995)).

Figure 10 – Tourmaline-bearing pegmatitic quartz veins possibly aligned parallel to the F4 axial plane (station JF13-38-012: UTM 495496 m E, 6299069 m N).

northern mapping area along several other unnamed lakes (Figure 2A). The fault zone is poorly exposed as it is largely in topographic lows that are in part occupied by lakes. The Burbidge Lake shear zone, which is several tens of meters wide, is characterized by protomylonitic to minor mylonitic rocks. Local sigmoidal tension gashes and small-scale asymmetric folds noted by Ramsay and Graham (1970) indicate a dextral shear sense. A pervasive, steeply west-northwest–plunging tectonic stretching lineation is common (Figure 9; Delaney et al., 1995). Thus, at least two generations of movement have occurred; however, the timing of these events is unclear. The Burbidge Lake shear zone repeats the Janice Lake Formation to the southeast of it, and therefore vertical displacement is

believed to be constrained to the thickness of the Janice Lake Formation. The Burbidge Lake shear zone was traced throughout the northern map area and likely continues farther to the northeast. An increase in the abundance of sandstone and more mature conglomerates (unit JLro) east of the Burbidge Lake shear zone, may represent a more distal sequence of the Janice Lake Formation (Delaney et al., 1995).

D4 was relatively weak in the study area and had little effect on the northeast-trending regional fabric. This event involved northwest-trending, upright folding, and is expressed as a weak crenulation on F3, possibly seen within an antiformal F3 map-scale fold just north of Burbidge Lake (Figure 2B). No axial planar cleavage (S4) was found in the map area, nor across the eastern Wollaston Domain (Tran, 2001). However, F4 axial planes were suggested by Tran (2001) to be filled with late, tourmaline-bearing pegmatitic quartz veins. Possibly one of these veins was found north of Burbidge Lake (Figure 10). This deformation probably occurred during a period of regional cooling, and was accompanied by minor retrogression and alteration (Tran and Yeo, 1997).

D5 produced a widespread conjugate set of northeast- to northwest-trending brittle faults that crosscut all of the structures described above. These structures are defined by lineaments that correspond to topographic depressions. This faulting is associated with, and possibly forms part of, the regionally extensive Tabbernor fault system in northern Saskatchewan. Kinematic indicators along the faults predominantly show sinistral movement (Figure 11A); however,


Figure 11- Minor faults related to D5 deformation. A) Pegmatite dyke aligned 010°; fanglomerate of the Janice Lake Formation, showing sinistral movement (station JF-18-004: UTM 506773 m E, 6311115 m N); B) a set of minor dextral faults aligned 009° showing offset of pink pegmatite dykes (station JF13-27-010: UTM 511502 m E; 6311096 m N); and C) a set of minor faults showing dextral movement within unit JLro (station JF13-19-008: UTM 510107 m E, 6310055 m N).

dextral movement along micro-faults was also observed (Figures 11B and 11C). D5 may be related to the disruption of the accreted terrain collage of the Reindeer Zone during terminal post-collisional stages of deformation (Tran and Yeo, 1997).

6. Metamorphism With the exception of some late pegmatitic dykes, most units were regionally metamorphosed during two Hudsonian metamorphic events, M1 and M2. Textural relationships between the similar metamorphic mineral assemblages suggest M1 (1860(?) to 1816 Ma) began before the peak of D1 deformation and ended during D2 deformation and M2 (1816 to post-1800 Ma) was broadly coeval with, and outlasted, D3 deformation (Tran, 2001). The map areas are underlain by a wide variety of quartzofeldspathic sedimentary rocks, which are not good record keepers of metamorphic processes. Therefore, most previous metamorphic studies have focussed on pelitic rocks, as these rocks respond relatively well to changes in pressure and temperature and therefore are better suited record the metamorphic history.

The Janice Lake and Rafuse Lake formations, in the area north of Janice Lake, were metamorphosed to lower amphibolite facies during M1. The presence of staurolite, garnet, biotite, hornblende, and andesine-oligoclase in the various units around Janice Lake caused Rath (1969) and Scott (1973) to suggest low-pressure intermediate-grade metamorphic conditions. Local partial melts are found within the arkoses and fanglomerate of the Janice Lake Formation possibly associated with M2 suggesting middle to upper amphibolite facies.

A B

C


At Burbidge Lake, metamorphic grade reached upper-amphibolite facies as indicated by the stability of sillimanite, cordierite, and K-feldspar with the apparent absence of muscovite along with partial melts within the pelitic rocks. Differing mineral orientations indicate that two distinct generations of sillimanite, cordierite, and K-feldspar developed during the M1 and M2 events. Cordierite partially or fully replaced sillimanite at some localities. K-feldspar–rich magmatic leucosome generally contains coarse-grained cordierite associated with M2.

7. Exploration History The exploration history of the area was compiled from the Saskatchewan Mineral Deposit Index (SMDI) where more detailed information can be found in regards to the copper showings. Other information can be found within assessment reports, which can be assessed through the Saskatchewan Geological Survey website. The first reported discovery of base metals in the Wollaston Domain was in 1953, by Simon Eninew who, while prospecting for E.F. Partridge, discovered a malachite-stained, chalcocite-bearing boulder just northeast of Janice Lake along the Wathaman River. It was not until 1966 that Great Plains Development found copper mineralization in place around Janice Lake. From 1962 to 1978, various companies including E.F. Partridge, Falconbridge Mines, Great Plains Development Co. of Canada Ltd., Newmont Mining Corp. of Canada Ltd., Wollex Exploration Ltd., and Giant Yellowknife Mines discovered several boulder trains and showings, mostly in an isolated area around Janice Lake including: Janice Lake (1966; SMDI #1016), Janice Lake North (1966; SMDI #1016), Kaz (1966; SMDI #1017), Zap Lake (1966; SMDI #1020), East Burbidge (1967; SMDI #996), “A” Lake (1968; SMDI #1021), Rafuse (1969; SMDI #1018), Lily (1969; SMDI #997), Howe Lake (1973; SMDI #1022), Kwest (1974; SMDI #1022), Breezy (1974; SMDI #1019a), and Zed Lake (1976; SMDI #998) showings. From 1991 to 1997, Noranda Exploration and Mining Ltd. carried out several geophysical, prospecting and drilling programs that resulted in the discovery of a number of additional copper occurrences both in boulders and outcrop including: the JS (SMDI #2632), JS2 to 4 (SMDI #996), RS1 to RS3 (SMDI #998), Genie (SMDI #2664), and Sunshine (SMDI #2665)showings. In 1994, Gary Delaney, with the Saskatchewan Geological Survey discovered the Jansem 1 and 2showings (SMDI #2632), while undertaking geological mapping in the Janice Lake area. From 2002 to 2007, Phelps Dodge Corp. of Canada discovered four additional copper showings: JL-2 (SMDI #996), Mackenzie(SMDI #2665), JL-1 (SMDI #996), and Roberts (SMDI #2665). In 2008, work was conducted by Resource EyeServices Inc. on behalf of Uracan Resources and Bonaventure Enterprise, targeting uranium in granitic intrusionsand pegmatite. In 2012, Transition Metals staked a group of dispositions in the Janice Lake area to further evaluate the area’s copper potential.

To the south of Janice Lake and to the east of Rafuse Lake a total of seven boulder showings and 22 bedrock showings have currently been discovered. These showings all occur in the area mapped by Delaney et al. (1995).

Although many of the copper showings in the Janice Lake area were visited during the current field program no new showings were noted within the areas mapped in the summer of 2013.

8. Economic Geology The Wollaston Domain has long been known to host copper mineralization (Rath, 1969; Scott, 1973; Coombe, 1977, 1994; Potter, 1977, 1978, 1980; Coombe Geoconsultants Ltd., 1991; Delaney 1993, 1994; Fossenier et al., 1994; Fossenier, 1995; Purser and Delaney, 1994; Delaney et al., 1995, 1996, 1997; Tran and Yeo, 1997; Delaney and Savage, 1998; Beaudmont, 2003; Yeo and Delaney, 2007). Historically, the origins of these copper occurrences have been variously interpreted as being of syngenetic (Rath and Morton, 1969), hydrothermal (Scott, 1973), or diagenetic origin (Coombe, 1994). The currently accepted model is that the copper occurrences are sediment-hosted stratiform copper deposits (Delaney, 1994; Delaney et al., 1995; Delaney and Savage, 1998).

For sediment-hosted stratiform copper deposits, the mineralizing process typically involves movement of oxidized, copper-bearing fluids through permeable strata, until they encounter a structural trap and/or reducing zone/horizon (Hitzman et al., 2005). For many model deposits, metal sources are believed to be red-bed sedimentary rocks (ibid.), therefore suggesting the arkoses of the Burbidge Lake Formation, from which the fanglomerates are derived and/or the fanglomerates themselves are the possible metal sources.

Basin geometry and basin evolution probably played a major role in the distribution of the Janice Lake copper occurrences, of which more than 20 are hosted either in fanglomerate of the Janice Lake Formation or in the overlying Rafuse Lake Formation. Many of the copper occurrences appear to be at or near the contact between the Rafuse Lake and Janice Lake formations, which may be have acted as a reducing horizon. The showings along this contact occur as irregular, patchy concentrations or stratiform occurrences (Delaney and Savage, 1998). Copper mineralization within the Janice Lake fanglomerate, including Jansem 1 and 2 and JL 1 and 3, appears to lack the presence of any noticeable reductive horizons, however, reduced zones within the fanglomerate area displayed by the lack of hematization around the Jansem 2 showing.


Economic minerals in the Janice Lake area include copper, chalcocite, malachite, azurite, antlerite, bornite, chalcopyrite, and bornite, occurring as clots and disseminations along fractures and as coatings on weathered surfaces (Coombe, 1994; Delaney et al., 1995; McGowan et al., 1997). The mineralized zones, and the immediately associated rocks, are weakly magnetic. Chlorite appears to be slightly more abundant in and near the mineralized zones.

Sediment-hosted stratiform copper deposits are common around the world, but economically significant deposits are rare (Hitzman et al., 2005). The abundance of small, and in some cases high-grade, showings in the Janice Lake area suggests favourable conditions for the formation of these types of deposits, particularly in the Janice Lake and Rafuse Lake formations. As mapping this past summer has traced these favourable units 15 km to the northeast, that area should also be evaluated for its potential to contain additional occurrences of sediment-hosted stratiform copper mineralization.

9. Discussion and Conclusions

a) Depositional Environment U-Pb data from detrital zircon collected throughout the Wollaston Supergroup indicate a depositional age for the sequence ranging from 2.07 to 1.86 Ga (Tran et al., 2008). A U-Pb age of 2075 ±2 Ma from detrital zircon in the Courtney Lake Group provides the maximum age for the onset of Wollaston Supergroup sedimentation (Yeo and Delaney, 2007), and deposition is thought to have ceased with emplacement of the 1.87 to 1.86 Ga Wathaman Batholith (Tran et al., 2008). Field relationships observed by Tran et al. (1998), Tran ( 2001), and Delaney et al. (1995) suggest that the upper Wollaston Supergroup was deposited in an active tectonic setting, when the southern Hearne craton margin was evolving from a back-arc basin to a foreland basin. The Daly Lake and Geikie River groups within the map area were deposited in the foreland-basin stage. Therefore, the formations within the map area have been interpreted to be deposited in fluvial-alluvial, and restricted marine to lacustrine environments (Tran, 2001).

Within the fanglomerate, there is a predominance of arkosic clasts and arkosic matrix; detritus of which was possibly derived from the underlying Burbidge Lake Formation, which consists of arkoses and quartzites. Thus, the presence of the fanglomerate suggests the existence of an actively uplifting paleoenvironment. Yeo and Delaney (2007) attributed the inferred uplift to imbrication caused by craton-verging thrust faults resulting from an advancing tectonic load.

A contrasting view is that of Beaudemont (2003), who suggested that the fanglomerate is composed of in situ breccias and pseudo-fanglomerates that formed as a result of felsic metasomatism during tectonism. Beaudemont’s arguments supporting a non-sedimentary origin include: 1) the presence of fine-grained cobbles within fragments; 2) the difficulty in distinguishing matrix and fragments within the same bed; 3) the homogenous composition of the fragments; and 4) the unusually large thickness of the fanglomerate/debris flow given its highly deformed nature. Based on the current mapping, however, it is suggested that the fanglomerate has undergone later deformation, which could have caused brecciation and reworking of the fanglomerate. It is believed that many local thrust faults could have caused reworking of the fanglomerate, particularly during late D3 when the Burbidge Lake shear zone developed. Within the fanglomerate there are rare pebble- to cobble-sized, sub-rounded, granitic, calc-silicate, amphibolite(?) and quartz clasts in some outcrops, which also supports a sedimentary origin for this unit.

The quartz pebble conglomerates (RLo) found just north of Burbidge Lake could also be derived from the Burbidge Lake quartzite (Figure 5) and have been previously interpreted as channel deposits related to deltaic sedimentation (Tran and Yeo, 1997).

Coarse siliciclastic sediments, including fanglomerate, conglomerate, and associated units within the Janice Lake Formation are found intermittently in the throughout eastern part of the Wollaston Domain, with the most extensive occurrence in the Janice and Burbidge lakes areas. A fold closure of a correlative unit to the fanglomerate is shown by Tran and Yeo (1997) southeast of Burbidge Lake and currently marks its southern extent; a lateral facies change west of Nelson Lake marks its northern extent. Therefore, fanglomerate and associated conglomerates have a minimum strike length of 35 km with a local apparent thickness of generally between 1.4 and 2 km, however, the true thickness is probably less as it is probably structurally repeated by folding and a series of northeast-trending thrust faults. The Burbidge Lake shear zone was traced throughout the northern map area and likely continues farther northeast.

The mapped sedimentary rocks containing units r2, r3, and rq along the western margin of the Janice Lake area appears to be in a stratigraphically higher position than the arkoses and arenites of the Rafuse Lake Formation; however, they are compositionally quite similar. It is presently unclear whether these units are stratigraphically distinct from the Rafuse Lake Formation or thrust slices.


b) Structure Many of the previous exploration companies have noted a high degree of difficulty when attempting to correlate drill holes due to both facies changes in the sedimentary succession and the effects of deformation. Polyphase folding and faulting are believed to be the main factors responsible for the lack of continuity of the mineralization. Across the map area, the fanglomerate displays a wide variation in clast size, clast shape, clast to matrix ratios, and matrix composition. These variations could be attributed to lateral facies changes because within an alluvial fan model, compositional variations are expected; however, differential strain also explains some of the observed variation particularly that resulting from the pervasive F3 and S3 fabrics. Due to the style of F3 folding, the fold hinges remain relatively ‘low’ strain, whereas the limbs are thinned, causing clasts to be stretched and elongated. Along the fold limbs, previous S1/S2 foliations are re-aligned sub-parallel to parallel to S3 so that they are commonly indistinguishable on most outcrops. The limbs of the F3 folds are also common activation sites for local transcurrent and thrust zones. In suspected fold hinges, the strain is low and primary features such as crossbedding have been observed by previous authors (Scott, 1973; Delaney, 1994; Delaney et al., 1995; Tran and Yeo, 1997). Large, angular to sub-angular, boulder-size clasts are also visible in suspected fold hinges, some with internal laminations that appear to be randomly orientated (Figure 4C). However, in some outcrops, the internal laminations within the boulder-sized clasts could be aligned parallel to the F2 foliation.

Although on a broad scale the stratigraphy and structural framework has been established for the sedimentary successions, many details about both remain unresolved. The context of known mineral occurrences and their relation to basin structure and deformation history is still poorly understood. This information is needed to evaluate the present copper showings and the potential of the Wollaston supracrustal succession to host other mineral occurrences.

10. Future Work This year’s mapping will be combined with Delaney’s (1994 to 1998) work in the region to create a compilation map for the area extending from Burbidge Lake to Nelson Lake. The recent burn in Burbidge Lake area affords a perfect opportunity to extend detailed mapping to the south to find the southern extent of the Janice Lake Formation. To complement the mapping projects, a geochemical study would be beneficial, especially within the fanglomerate to determine whether the ore-forming processes have left a geochemical fingerprint. A B.Sc. thesis by E. Martyniuk of the University of Saskatchewan is being undertaken to characterize the petrography of the ore minerals and the chemical characteristics of the Jansem 1 and 2 showings.

11. Acknowledgements Field work was performed with the valuable assistance of Kate Houston, Evan Martyniuk, Billy Fan, Adam Edwards, Ravyn Godwin, and Jennifer Regier. Much gratitude is given to Michelle Hanson and the bedrock mapping geologists of the Saskatchewan Geological Survey for their patience and guidance. Field visits by Gary Delaney and Jason Berenyi were very helpful in improving the map and report. I would also like to thank Hal Sanders for an enjoyable field visit. Logistical support was provided by Osprey Wings and Thompson Camps in Missinipe, Saskatchewan.

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