A Systems Tract Approach to the Stratigraphy of Paragneisses in the Southeastern Wollaston Domain

Gary Yeo

Yeo. G. (1998): A systems tract approach to the stratigraphy ofparagneisses in the southeastern Wollaston Domain; in Summary of Investigations 1998. Saskatchewan Geological Survey. Sask Energy Mines. Misc. Rep. 98-4.

Isoclinally folded, upper amphibolite to lower granulite facies paragneiss units distinguished in recent detailed mapping in southern Wollaston Domain are interpreted to comprise two successive passive margin sequences and their component systems tracts. A major regional unconformity separating the two sequences may reflect the northwestward migration of a flexural bulge onto the margin of the Rae-Hearne Craton as the La Ronge volcanic arc advanced toward it.

1. Introduction The Wollaston Domain is a 60 to 80 km wide belt of gneisses overlying Archean granitic basement rocks along the eastern margin of the Rae-Hearne Craton. It forms part of the Cree Lake Zone, the external, western part of the Trans-Hudson Orogen. Except along the eastern side of the domain, interpretation of the gneisses is complicated by high metamorphic grade, complex deformation, and poor age constraint (2.1 to 1.85 Ga).

In 1997 a three-year, 1 :20 000 scale mapping project in the southern part of Wollaston Domain was begun (Figure 1). The project was initiated in the Burbidge Lake-Upper Foster Lake area (Tran and Yeo, 1997), where, locally, metamorphic grade is low and primary structures are preserved (i.e. Burbidge Lake area). Mapping in 1998 was carried out in the Daly Lake­Middle Foster Lake area (Tran et al., this volume). A basic strategy of the project is to map outward (up stratigraphy) from Archean inliers as much as possible. The purpose of the project is to improve understanding of the stratigraphy and structure of the Wollaston gneisses, which underlie the world-class, unconformity-type uranium deposits of the middle Proterozoic Athabasca Basin. With one important exception, these are associated with the basal Wollaston graphitic pelites (Saskatchewan Geological Survey, 1994). The Rabbit Lake deposit, however, is associated with calc-silicate rocks much higher in the Wollaston succession (Sibbald, 1976). rn addition, a number of base metal prospects are known in the southern Wollaston Domain. Zinc-lead occurrences are found in lower Wollaston quartzites in the Johnson River-Morell Lake (Delaney et al., 1996, 1997) and Foster River (Coombe, 1994; Delaney and Savage, this volume) areas, whereas copper is found in conglomerates and arkoses in the Janice Lake (Delaney, 1994; Delaney et al., 1995) and Duddridge Lake (Delaney, 1993) areas.

36

The purpose of this paper is to summarize observations of southern Wollaston Domain stratigraphy based on detailed mapping, and show how a systems tract depositional model can aid in the interpretation of these hi$h metamorphic grade, polydeformed paragne1sses.

2. Lithostratigraphy

Most of the major lithologic units mapped in the Burbidge Lake-Upper Foster Lake area can be correlated with those of the Daly Lake-Suttle Lake­Middle Foster Lake area (Table I). The units are only briefly outlined below, as they are described in more detail elsewhere (Tran and Yeo, 1997; Tran et al., this volume). For the purpose of discussion, they are given mnemonic SEM map codes in this report since the map unit numbers of correlative units in the two areas do not correspond.

a) Basement Rocks

In contrast with the overlying metasedimentary rocks, the basement rocks in the two map areas are different. In the Upper Foster Lake area, basement is exposed in the Karin Lake Inlier, a concentrically zoned granitic complex. Xenoliths of quartzite, arkose, biotite psammite, and amphibolite are especially common in granodiorite-tonalite and late pegmatite of the marginal zone. Amphibolite sheets intrude the basement rocks, but not the overlying metasedimentary rocks. Ray ( 1977) interpreted yellow-white zones in the Karin Lake Inlier as possible evidence ofpaleo-weathering. White, cordierite-muscovite-sillimanite schist at the southwest margin of the inlier was interpreted as a meta-regol ith by Annesley and Madore ( 1991 ).

rn the Daly Lake area, basement is exposed in the Roper Bay and Pederson Lake inliers, which are unzoned granodiorite to quartz monzonite complexes containing bodies of charnockitic quartz monzonite. As at Karin Lake, there is a marginal zone in which late pegmatite, with metasedimentary enclaves, predominates. Amphibolite sheets and boudins in these marginal rocks are not found in the overlying metasedimentary succession.

The age of the Karin Lake and Roper Bay inliers is not known, but a Rb-Sr whole rock age of 2500 Ma has been reported from the Pederson Lake Inlier (Bell and Macdonald, 1982). This is consistent with U-Pb zircon ages for basement elsewhere in the Wollaston Domain

Summary of Investigations 1998

b

a

Saskatchewan

200 km

I [lmJ J Burbidge L. - Upper Foster L. area ........_ Major fault or shear zone

Daly L. - Middle Foster L. area Lake

[I ··;· ··i .. . . -· . j ••••

Phanerozoic sedimentary rocks

1.35-1.8Ga sedimentary rocks

1.6-1.8Ga intrusive rocks

1.6- 1.8 Ga volcanic and sedimentary rocks

1· . - ' 1.8 - 2.1 Ga '. ·.: ·: · 1 intrusive rocks

t' '""' .... " " .... vi .,-v v v , ,,, ... "" v

v" " '!'J

• ~@j [""""!

L:.:.:::::1

1.8-2.1 Ga volcanic and sedimentary rocks

1.8- 2.5 Ga sedimentary rocks

2.1 - 2.8 Ga intrusive rocks

2.1 - 2.8 Ga volcanic and sedimentary rocks

> 2.5 Ga undifferentiated rocks

LEGEND

Athabasca Basin

Sandstone and conglomerate

Mudjatik Domain

l/ /I Felsic gneiss with minor .,- .r metasediments and volcanics

Wollaston Domain

I~ I I

•

Granitoid intrusives

Janice Lake Conglomerate

Undifferentiated metasedimentary rocks

Felsic gneiss

Peter Lake Domain

1':j\1 F~ls.ic - mafelsic plutons, f,s / J d1orite, and gabbro

Wathaman Batholith

: : : ; : Monzogranite (1.85Ga) .. ' Rottenstone Domain I;; ; ] Biotite and hornblende gneisses l;__;_:;j and trondjhemite-tonalite

Figure I - a) Location map of the 1.8 to 2.1 Ga Wollaston Domain and related rocks (the area of lb is outlined). b) Location map of the Burbidge Lake-Upper Foster Lake and Daly Lake--Middle Foster Lake areas in southern Wollaston Domain.

Saskatchewan Geolog ical Survey 37

(e.g. Ray and Wanless, 1980). The age of the sheet-like arnphibolite intrusions is also unknown, but since they post-date Archean basement and pre-date the cover strata, they may be correlative with the Courtenay Lake volcanics, dated at 2.1 Ga (Delaney, pers. comm.

upper part of th is unit lacks garnet and is transitional into the overlying Unit Wnps.

1998), and interpreted to mark the initial rifting of the Rae-Hearne Craton and the onset of Wollaston sedimentation (Fossenier et al., 1995).

c) SilJimanite-cordierite-bearing Psammopelite, Pelite, and Psammite (Unit Wnps)

b) Garnet and Graphite-bearing PeJites, Psammopelites, and Quartzites (Unit Wna)

The basal unit comprises thinly interbedded gamet­cordierite pelite, psammopelite, and psamm ite. Around the Karin Lake Inlier it is psammite-dominated, and typically graphitic, whereas, adjacent to the Roper Bay Inlier, petites predominate and graphite was not apparent, although Ray ( 1981 ) noted its presence in this area. Annesley and Madore (1 99 1) reported "fine to coarse-grained, well-layered, gametiferous, and hematite-rich" banded iron format ion associated with the basal pelites at the northern margin of the Karin Lake Inlier. Banded, garnet-rich rock in Unit Wna at the north end of Lower Foster Lake and in the Sito Lake area is interpreted as sil icate facies iron formation (Poner, 1980; Delaney and Savage, th is volume). The

Si llirnanite-cordierite bearing, thin-bedded psammopelite and petite with abundant, augen-like, feldspath ic melt lenses is found in the eastern part of both map areas. Arkos ic psammite is also present in the lower part of this uni t in the Burbidge Lake area. The melt lenses typical of this unit are feldspar-rich ovoids or d iscs up to several centimetres long, commonly containing sillimanite and/or cordierite, and with biotite selvages. The format ion of the melt lenses likely involves metamorphic dehydration reactions (e.g. Kerrick, 1988; Nabelek, 1997). This unit is transitional into overlying Unit Wns. It is absent to the west in the Upper Foster Lake area, and th ins westward in the Daly Lake area.

d) Magnetite-bearing Psammopelite to Pelite (Unit Wns)

Predominantly homogeneous psamrnopelite to psammite, locally containing

Table 1 - Correlation between map u11its distinguished ill the Burbidge Lake- Upper Foster Lake and Daly Lake- Middle Foster Lake areas and those used in this report.

sillimanite or cordierite, and accessory magnetite, is interbedded with minor quartzite and/or arkose This unit is found in the western part of both areas and may be a facies equivalent of Unit Wnps. It is transit ional to overlying Unit Wnsp.

Daly - Suttle - Middle Foster Burbidge - Upper Foster Lakes Lakes area 0998 mao units) area II 997 mao units) UPPER SEQUENCE UPPE R SEQUE NC E

13. Cale-sil icate rocks 17. Dolomit1c marble 16. Cale-silicate rocks

12. Cale-silicate-bearing arkosc 15. Cale-silicate-bearing arkose

14 . Muscovite schist

11 . Con2lomcrate 12 . Conglomerate & arkose unconformitv unconformiry LOWER SEQUENCE LOWER SEQUENCE

10. Quartzite 13. Arkose 9 . Arkose 8. Banded biotitc gneiss I I . Banded biotitc gneiss

7. Biotite psammopelitc to 10. Biotitc psammopelitc osammite 6. Silhmanitc-cordicrit~bearing 9. Sillimanite-cordierite>-bcaring biotitc psammopelites and pelites biotite psammopclites and pelitcs with fe lsic melt lenses with fclsic melt lenses

8. Arkosic psammitc to osammooelite

5 . Gamet-cordierit~ bearing 7. Graphitic biotitc petite biotite pelite and psammopelite 6 Graphite-garnet· bearing biotite with nuartz1te interbeds oelite and semipelitc ROPER BAY AND KARIN LAKE BASEMENT PEDE RSON LAKE COMPLEX BASEME NT COMPLE X 3. Amphibo hte 5. Amphibolite

4. Marginal assemblage· 4. Marginal assemblage: deformed diorite-tonalite and pegmallte and grandodiorite to undeformed pcgmatite with tonalitc with mctasedimcntary metasedimentary xenoliths xenoliths l - 2. Granitic rocks includ ing I - 3. Granitic rocks chamockite ···-------- .•.

38

··-Protolith and Interpret at ion

Lowstand and transgressive svstems tracts Wn c: Salina or restricted basin calcareous sediments & evaoontes Wrnc: Carbonate-cemented coastal sands Wnp: Mudstone (near Burr orosoect) Wo: Alluvial fan deposits Re11.1ona/ uplift Transgressive and highstand svstems tracts Wrn: Coastal sands

Wnsp: Transitional shelf sands and muddv sands Wns: Shelf muddy sands

Wnps: Outer shelf muddy sands and sandy muds

Wna: Shelf muds and sands

Basement rocks

Possibly mafic dykes associated with earlv Wollaston riftinR Metasediments may be remnants of a pre-Wollaston platform succession

Probable Archean orthogneisscs

e) Banded Biotite Gneiss (Unit Wnsp)

Thin to thick interbedded arkose, psammite, and biotite psammopelite, typically with abundant magnetite and/or calc­silicate minerals, underlie both areas. It is transitional to overlying Unit Wm.

f) Arkose (Unit Wrn)

Banded or massive pink arkose, locally with calc-silicate or psammopelite interbeds, is found in both areas. Quartzite locally overlies or interfingers with it in the Daly Lake area. It is at least 250 m thick in the Burbidge­Upper Foster lakes area (Tran and Yeo, 1997, Figure 3).

Summary of Investigations 1998

g) Janice Lake Conglomerate (Unit Wo)

Polymictic ortho- and paraconglomerates with intercalated arkose beds are restricted to the eastern part of both areas. North of Burbidge Lake their thickness is up to 1.4 km, although their original thickness may be less (Delaney et al., 1995). The composition and texture of the conglomerates are locally variable. Metasedimentary clasts (arkose and quartzite) predominate, although granitoid and quartz clasts are locally common. Pebbles and cobbles predominate, but boulders are locally preserved. Clasts range from subrounded to angular. The conglomerate matrix is calcareous arkose. In both areas, the conglomerates are laterally and vertically transitional to arkose or calcareous arkose.

h) Muscovite Schist (Unit Wnp)

This thin muscovite schist was recognized only in the vicinity of the Burr uranium showing east of Burbidge Lake.

i) Cale-silicate-bearing Arkose (Unit Wrnc)

Cale-silicate-bearing arkose, with up to 10 percent diopside and/or hornblende, and accessory ilmenite, rather than magnetite, is widespread in both areas. North of Burbidge Lake, it is at least 200 m thick (Tran and Yeo, 1997, Figure 3). It is typically well-bedded, with minor interbeds of quartzite, arkose, calc-silicate rocks, and plagioclasite.

This unit is locally in contact with all of the underlying rock units; hence its base is either a thrust fault or an unconformity. There is no evidence for thrust faulting at this contact. An angular unconformity is indicated by: (a) the conglomerate underlying Unit Wrnc, which must have been deposited following uplift (discussed below); (b) the truncation of contacts between underlying units by Unit Wrnc west of the Karin Lake Inlier; and (c) local erosion of the underlying strata.

j) Cale-silicate Rocks (Unit Wnc)

Cale-silicate rocks, with more than IO percent diopside and/or hornblende, and accessory ilmenite, are commonly associated with or overlie the calc-silicate­bearing arkosc. They include white and green banded diopside-rich arkose, plagioclase-diopside breccia, pegmatite-like plagioclasite, and amphibolite. Dolomitic marble is locally present.

k) Intrusive Rocks

Small bodies of hornblende gabbro, coarse crystalline plagioclasite. and granite pegmatite intrude the metasediments in both areas. The Suttle Lake Complex, a large intrusive complex between Suttle Lake and Middle Foster Lake, comprises sheets of diorite-quartz diorite and granite-granodiorite-tonalite with xenoliths and screens of metasediment. The complex underwent D2 folding and hence was probably emplaced during D

1 deformation.

Saska1chewa11 Geological Survey

3. Structure and Metamorphism

The rocks of the southern Wollaston Domain have undergone at least four episodes of deformation and two of metamorphism (Tran and Yeo, 1997; Tran et al., this volume).

D 1 involved isoclinal folding. S 1 foliation is common, but typically reoriented parallel to S2• Minor F 1 folds are rare. 0 2 involved open to isoclinal refolding about northeast-trending, steeply northwest dipping axial planes. This produced the dominant regional structural grain. 0 3 involved very open folding about near­vertical, northwest-trending axial planes. D4 involved faulting along northerly to northwesterly trends, typically with sinistral offsets. Due to isoclinal fold repetition and high strain, the original thickness of lithostratigraphic units, except for the relatively competent conglomerates and arkoses, cannot be determined.

M 1 is associated with D 1• M 1 metamorphic mineral assemblages include sillimanite, cordierite, garnet, and K-feldspar, suggesting P-T conditions of 4 to 5 kbar and <750°C. M2 is associated with 0 2. M 2 metamorphic mineral assemblages are the same as those ofM 1, but include hypersthene. This suggests peak P-T conditions of 5 kbar ( 15 to 18 km burial) and 750° to 780°C. Due to metamorphism (and high strain), primary sedimentary structures, except for compositional layering, are generally not preserved.

4. Sequence Stratigraphy

The application of seismic stratigraphic interpretation methods to the analysis of sedimentary basins in the 1970s and 1980s (Vail et al. , 1977; Vail, 1987; and others) led to the development ofa new way to subdivide and correlate strata known as sequence stratigraphy (Walker, 1992; Christie-Blick and Driscoll, 1995; and others). Although sequence stratigraphy was initially developed to interpret seismic sections, it is now commonly applied without reference to seismic data ( e.g. Suchy and Steam, 1992; Glover and McKie, 1996; Schenk, 1997; and others).

A sequence is an essentially conformable assemblage of genetica\ly related strata bounded by unconformities and their corresponding conformities (Mitchum, 1977; Yan Wagoner et al., 1987). A sequence, in tum, may be subdivided into parasequence sets or systems tracts. Boundaries between systems tracts are conformable. A systems tract generally contains several lithofacies, but they are genetically related (i.e. facies equivalents) and deposited within the same time interval (i.e. chronostratigraphic equivalents). Each type of systems tract is deposited by a particular set of depositional processes, and thus distinctive depositional environments and lithofacies are associated with them. Systems tracts have predictable relationships and facies patterns; hence, they provide a framework to relate mapped lithofacies in space and time and more accurately identify their depositional environments and processes (Figure 2). Systems tracts

39

are the basic building blocks of sequence stratigraphy. They can be subdivided in tum into parasequences, conformable successions of beds, laid down in related facies belts. Individual parasequences are progradational and, hence, shoal upward (Van Wagoner et al., 1987).

The underlying basis of sequence stratigraphy is the interplay between relative sea level change and sediment supply. Relative sea level change governs the 'accommodation space' in which sediment may accumulate, and is a combination of eustatic sea level change and tectonic subsidence. The fundamental control on depositional sequences is short-term eustatic sea level change, superimposed on long-term tectonic subsidence and uplift.

Four types of systems tracts can be distinguished. If subsidence and sediment supply remain constant, the

type that forms depends on eustatic sea level fluctuation.

Eustatic sea level rise causes transgression and a retrogradational (landward) shift in the sedimentary depocentre and facies belts. The resulting deposits belong to a transgressive systems tract (TST). The parasequences that comprise a TST thin and fine seaward and upward due to sediment starvation. Hence TSTs thin seaward overall, and their seaward part is a condensed section. The boundary between a TST and an overlying highstand systems tract represents the maximum extent of marine transgression, the maximum flooding surface.

A period of stable eustatic sea level following a transgression causes sediment and facies belts to prograde seaward. The resulting deposits belong to a highstand systems tract (HST). In contrast with

TSTs, HSTs coarsen upwards.

correlative conformity (sequence boundary)

If eustatic sea level falls, regression and a progradational (seaward) shift in facies belts results. The resulting deposits belong to a lowstand systems tract (LST). These accumulate seaward of underlying systems tracts, and pinch out landward, except where their deposits fill valleys incised in underlying strata.

__ ooooofomity ---,,_ -~c.-;_S~§T°''T--,. __ .. l -~-~~~~=~·~:~~--~~i~~:~~~~~~~: ~ """'"fomity-~'i;;~:~~~:.:;;ii\1';; ,: ;;i~i~i,Jiff i r

correlative conformity (b) In Geologic Time (sequence boundary)

FACIES

:-:·>I Alluvial

I:":' Coastal Plain

liJ Estuarine/Fluvial :·. f;i:·;·~i

(\! Shoreface/Deltaic Sands ...

f=f ~ Marine Muds ~-:-:J ·:-:·" Deep-water Sands

SYSTEMS TRACTS

HST Highstand Systems Tract

TST Transgressive Systems Tract

LST Lowstand Systems Tract

SMST Shelf Margin Systems Tract

Figure 2 - Sequence stratigraphy diagrammatic section showing the typical distribution of siliciclastic sediments within sequences and their constituent .\ystems tracts in depth and time (after Vail, 1987, Figure 4).

40

If the rate of subsidence is greater than the rate of eustatic sea level drop following a highstand, the sediment depocentre and facies belts remain fixed or shift slightly seaward and an aggradational parasequence set results. This is a shelf margin systems tract (SMST), which pinches out landward.

Although sequence stratigraphy has become a standard technique for analysis of unmetamorphosed platform and craton margin strata (e.g. Suchy and Steam, 1992; Morton and Suter, 1996; Carey et al., 1998: and many others), and has been confirmed on modem sedimentary environments (e.g. Boyd et al., 1989), there are few examples of its application to metamorphosed and deformed strata (e.g. Glover and McKie, 1996; Schenk, 1997).

Summary of Investigations 1998

5. A Sequence Stratigraphic Interpretation of the Daly Lake-Foster Lakes Paragneisses

Previous workers recognized the probable protoliths of various lithologies and interpreted the Wollaston paragneisses as a miogeosynclinal or passive margin succession (Money, 1968; Money eta!., 1970; Ray and Wanless, 1980; Lewry and Collerson, 1990; and others). They recognized that: (a) granitic inlier rocks show that the Wollaston sediments accumulated on cratonic basement, (b) abundant compositionally immature sediments (e.g. arkoses and wackes) indicate a subsiding basin, and (c) lateral continuity of lithologic units and the widespread distribution of pelitic rocks indicate a predominantly marine environment, although conglomerates and probable evaporitic sediments suggest periods of emergence. It was not until the initiation of detailed mapping projects in the Wo\laston Domain (Delaney, 1993), however, that attempts were made to infer the depositional setting of individual lithologic units.

The interpretation of ancient sedimentary rocks has traditionally been based upon comparison with modern sedimentary environments and the application of facie s models (e.g. Walker, 1992). Stratigraphic interpretation of the Wollaston metasediments, however, has been

West

inhibited by limited detailed mapping, and high-grade metamorphism and deformation, which have generally obliterated primary features. Since passive margin sedimentation is controlled mainly by eustasy. rather than tectonics, the Wollaston paragneisses ought to fit into a sequence stratigraphic framework.

There are three steps in applying sequence stratigraphy to a lithostratigraphic succession. The first step is to identify the major unconformities or sequence boundaries. The second is to match the packages of mapped lithostratigraphic units to the appropriate systems tracts by recognition of transgressive and regressive facies trends within those packages. The third is interpretation of the depositional environments of the lithostratigraphic units.

a) Sequence Boundaries

Two major sequence boundaries subdivide the succession in the Daly-Foster lakes area. The basal unconformity above Archean basement can be recognized without difficulty. Xenoliths of metasediment within the basement inliers generally cannot be matched with strata above this unconformity, and hence, probably pre-date it. Furthermore. amphibolitc sheets intruding the marginal rocks of the

basement inliers do not cut

East Janice Lake Conglomerate

i overlying rocks. The xenoliths may be remnants of a pre-rift early Proterozoic or Archean platform assemblage.

(a) In Depth (lithostratigraphic units indicated)

(b) In Geologic Time (systems tracts indicated)

I 1-[L UJ 0

l w ~ 1-

1 Figure 3 - Sequence stratigraphic interpretation of the southern Wollasto11 Domain paragneisses. (a) Schematic /ithostratigraphic section viewed from the south showing the lithologic units corre.\ponding to each of the systems tracts outlined in this report. (b) Schematic chronostratigraphic section showing the systems tmcts corresponding to the assemblages of lithologic units comprisin,: each one. Sy.flems tract andfacie.f symbols are as in Fi,:ure 2.

Saskatchewan Geological Survey

The base of the Janice Lake Conglomerate marks a second unconformity, first recognized by Delaney and others ( 1995) at Janice Lake. To the west, where the conglomerate is absent, this unconformity corresponds to the base of the calcareous rocks that overlie it. Recognition of this unconformity at Daly Lake" shows that it is a regional feature. Within each sequence, the mapped lithofacies units can be assigned to a succession of systems tracts (Figure 3 ).

b) Lower Sequence

Within Unit Wna, graphitic wacke fines upward to mudrock in the Upper Foster Lake area. Such a retrogradational pattern is consistent with a TST. Intercalated, generally thin, sandy and muddy layers in Unit Wna might be interpreted as either thin-bedded turbidites or stom1 deposits intercalated with shelf muds and muddy sands. The latter interpretation is favoured because these beds Jack the well-developed grading

./ I

typical of classical turbidites, even at high metamorphic grades, and because a transgressive shelf setting is more likely than a shelf-edge fan setting for the basal unit of a sedimentary succession deposited directly on basement rocks. The sand layers were probably deposited from storm-generated flows, whereas the muddy layers were probably a combination of storm-generated sediment and background pelagic suspension deposits (Walker and Plint, 1992). Intercalated thin sand and mud layers are typical of a distal transgressive shelf setting, whereas intercalated thick sands and muds are more typical of a proximal setting (Zhang et al., 1997). Graphite in these rocks indicates anoxic conditions, typical of shelves where upwelling (Demaison and Moore, 1980) or rapid transgression, characteristic of early rift ocean margins, takes place (Arthur and Schlanger, 1979). The seaward part of this systems tract probably represents a condensed section, starved of elastic input. Such conditions favour accumulation of chemical sediments such as the lean iron formation reported locally from Unit Wna.

Mudrocks, wackes, and ferruginous wackes of Units Wnps and Wns coarsen upward into litharenite and arkose of Units Wnsp and Wm, consistent with a HST. The high alumina content indicated by sillimanite and cordierite in Unit Wnps suggests a clay-rich protolith, and hence a relatively quiet, deep water setting. Unit Wns is probably facies equivalent to Unit Wnps. The relative scarcity of aluminous minerals in Unit Wns indicates a more proximal setting. Units Wns and Wnsp are interpreted to be inner and outer shelf deposits respectively. The absence of graphite and increased magnetite content, in these units, particularly Unit Wns, suggest less anoxic conditions. Units Wnsp and Wm are likely distal and proximal shoreface sands (Walker and Plint, 1992) respectively.

c) Upper Sequence

The Janice Lake Conglomerate (Unit Wo) and associated arkose indicate a period of uplift, and possibly extensional faulting. Such sediments do not fit easily into a sequence stratigraphic model because they result from tectonism rather than eustasy. They are interpreted as LST deposits, since relative sea level must have fallen dramatically at this time. This explains their restriction to the eastern part of the Wollaston Domain, near or at the ancient shelf edge. Delaney and others ( 1995) interpreted the well­preserved conglomerates and associated arkose north of Burbidge Lake to be alluvial fan and associated braided river deposits deposited in an arid climate. Here, facies relationships indicate it was shed eastward (Delaney et al., 1995). Variable clast sorting and rounding, interbedding of orthoconglomerate and sandstone (stream flow deposits) and sandy paraconglomerate (debris flow deposits), and lateral and vertical transition to finer grained facies (calcareous arkose) observed east of Daly Lake (Tran et al., this volume) are also typical of alluvial fan deposits (Nilsen, 1982; Collinson, 1986). Low matrix mud content and debris flow deposits suggest an arid

42

environment (Kochel and Johnson, 1984, Table I; Collinson, 1986).

The calc-silicate-rich rocks (Units Wrnc and Wnc) that cap the sequence include mudrocks, arkose, and diopside-rich rocks (possibly evaporites originally). Although relationships among the assorted calc­silicate-rich facies of Unit Wnc are generally unclear, the characteristic presence of Unit Wmc below them indicates overall upward fining, at least in this part of the succession. Hence, these strata are interpreted as a TST, at least in their lower part. An overlying HST may also be present, but cannot be clearly distinguished. The calcareous arkoses of Unit Wmc are interpreted as braided river to coastal sands. Calc­silicate-rich layers in the arkoses may reflect episodic flooding. The calc-silicates of Unit Wnc are interpreted to be evaporites, marls(?), and minor dolostones deposited in a restricted basin (e.g. Schreiber, 1986; Kendall, 1992). Compositional layering in these sediments suggests cyclic deposition.

Although calc-silicate minerals are common throughout the Wollaston succession, their increase in the upper sequence must reflect a major change in the regional sedimentary regime. Clastic supply was probably reduced over time, as the flexural bulge, inferred to have caused faulting and deposition of the Janice Lake Conglomerate ( discussed below), migrated onto the craton. Precipitation of carbonates and evaporites support the inference above that the climate was arid. This would also have inhibited chemical weathering on the craton and reduced the supply of elastic sediment, particularly clays. Deposition of the calc-silicates may have occurred in coastal salinas, comparable to those of South Australia (Schreiber, 1986) or possibly in a hypersaline basin formed between the flexural bulge and the converging volcanic arc (discussed below), analogous to the upper Miocene Mediterranean Basin (Schreiber, 1986).

Fragmental calc-silicate rocks comparable to the "pseudoconglomerate" reported southwest of the Karin Lake Inlier (Tran and Yeo, 1997) are common in the Middle Foster Lake-Suttle Lake area. They consist of pale pink to white, unsorted, angular to subrounded, plagioclase-rich (albitite) clasts in a greenish diopside­or hornblende-plagioclase matrix. A single quartz clast was observed. They have been interpreted as syndepositional solution breccias (Ray, 1981 ), or as tectonic breccias related to late intrusions such as the Suttle Lake Complex (Mawdsley, 1957). The clasts are commonly flattened parallel to S2, but are little deformed compared to those in Unit Wo conglomerates in the same area. Locally the fragmental rock is transitional to albitite with calc-silicate-filled fractures. These observations suggest that the rock is a fluidization breccia that formed during or after D2

deformation. The observed clast rounding was probably due to "milling" during brecciation. Since the Suttle Lake Complex intrusives were folded and foliated during D2 , it is unlikely that the albitite breccias are related to intrusive activity.

Summary of Investigations 1998

6. Regional Significance of the Janice Lake Unconformity

The Janice Lake Conglomerate and its correlatives can be traced for at least 245 km along the eastern edge of Wollaston Domain, from Hills Lake (Delaney et al., 1996) to Duddridge Lake (Delaney and Savage, this volume). It corresponds to a regional unconformity that can be mapped westward at the base of the associated calc-silicate-bearing arkose (Tran and Yeo, 1997; Tran et al., this volume). A correlative unconformity has also been reported from the Manitoba segment of the Wollaston Domain (Weber et al., 1975).

el al., 1995; MacNeil eta/., 1997), makes mechanical flexure more likely. A possible cause of this is tectonic loading of the eastern margin of the Rae-Hearne Craton by the La Ronge-Lynn Lake volcanic arc as it converged towards the craton above an east-dipping subduction zone(Figure 4; also see Ray and Wanless, 1980, Figure 5, and Lucas eta/., 1997, Figure!).

Uplift and crustal extension on a passive margin may result from either thermal doming or mechanical flexure. The absence of syndepositional igneous activity, except for the Courtenay Lake volcanics, which are interpreted to manifest initial rifting and formation of the Wollaston passive margin (Fossenier

Volcanism in the La Ronge-Lynn Lake arc began about 1910 Ma (Baldwin et al., 1987) and reached its peak about 1880 Ma. Following arc-craton collision at about 1860 Ma (Bickford et al., 1990; Lucas et al., 1997), the sense of subduction was reversed and the Wathaman Batholith was emplaced at about 1855 Ma (Bickford et al., 1986). Geochemical evidence suggests that the La Ronge segment of the arc developed in a transitional crust setting, mainly on oceanic crust, but close to or partly over marginal continental crust (Watters and Pearce, 1987).

"

1-,' ' .... ····-··-··

I ·i

Passive margin sedimentation

Loading of plate margin by advancing volcanic arc causes flexural bulge: uplift, normal faulting, Janice Lake sediments, and regional unconformity

~ ;, !)-~<-~~\2 i : f ~;·t~~r~:\~~~~t~{::;~f ~~:~~ ·_ , , ',, .-::, ,. 's • .. '; ·, 's .,_ , . ·"-, •. _·:. ~lIT,lJr,. ·-'~" __ ' ~ ~;:r~'; ;:f::;;r ~· ¥.':./ · · 1nrn1

I I I Flexural bulge

11111 1 (triangle) shifts I cratonward as I foreland basin I stage begins

[/~,;!,>W\~"i~~~*Wi~ Figure 4 - Effect of tectonic loading of the Rae-Hearne craton edge by the La Range Arc on Wollaston sedimentation prior to arc-craton ccllision, subduction reversal, and emplacement of the Wathaman Batholith (after Stockmal and Beaumont, 1987, Figure 4). Schematic cross-sections are viewed from the south. Random dash pattern=continental crust: vertical ruled pattern=oceanic crust: vee pattern=arc vo/canic.v; stipple pattern=platform margin sediments: and horizontal dash pattern=forearc and trench sediment.

Saskatchewan Geological Survey

Convergence of the volcanic arc terrane with the eastern margin of the Rae-Hearne Craton would probably have resulted in loading of the outboard craton margin and fonnation of an inboard flexural bulge (e.g. Stockmal and Beaumont, 1987), with consequent normal faulting and erosion over the crest of the bulge and deposition of coarse elastics on its flanks. As convergence proceeded, the bulge would have migrated cratonward and died out, creating a diachronous regional unconformity. Preservation of the coarse elastics would be favoured only on the outboard craton margin, however.

Analogues for the Janice Lake unconformity can be recognized in craton margin rocks in Phanerozoic Orogens. They include: (a) the pre-Fernie unconformity in the southern Canadian Cordillera, created by an easterly migrating flexural bulge in Triassic-Jurassic time, as the lntermontane Superterrane (Stikinia) converged with the passive margin of western North America (Stockmal and Beaumont, 1987); (b) the widespread, sub-Tippecanoe (Taconic) unconfonnity in the Appalachians, created by a westerly migrating flexural bulge in mid-Ordovician time, as a volcanic arc converged with the passive margin of eastern North America (Lash, 1987); and (c) the sub-Flysch unconformity in the Alps, created by a northerly

43

migrating flexural bulge in early Cretaceous to mid­Eocene time, as microplates converged with the passive margin of southern Europe (Stockmal and Beaumont, 1987). Note that in all of these cases collision and foreland basin sedimentation continued long after initiation of the flexural bulge on the platform.

As convergence proceeded, the volcanic arc would have become a barrier to the open ocean, and accumulation of evaporites and carbonates in the resulting restricted basin would have been favoured. Terrane convergence may also have driven mineralizing fluids updip to form the syndepositional base metal deposits of the southern Wollaston Domain.

A somewhat similar interpretation, suggested by Tran and others (this volume), is that arc-collision formed a high terrain east of the present Wollaston Domain. This not only acted as a marine barrier, but as a source for the upper sequence elastics, including the conglomerate. Facies relationships in the Janice Lake Conglomerate north of Burbidge Lake (Delaney et al. , 1995), and local removal of much of the strata below the unconformity west of the belt in which conglomerate is preserved (i.e. Units Wm , Wnsp, Wns, and Wnps), indicate uplift to the west; however, not the east.

7. Conclusions

This report shows how sequence stratigraphy can improve our understanding of the deposition of sediments ancestral to polydeformed, high-grade paragneisses. In a sequence stratigraphic framework, two depositional sequences, separated by a major unconformity, can be distinguished in the southern part of the Wollaston Domain.

The lower sequence comprises a TST, deposited under at least partly anoxic conditions, overlain by a HST, deposited under non-anoxic conditions. The upper sequence comprises a LST, represented by alluvial fan deposits restricted to the eastern part of the Wollaston domain, overlain by a TST that accumulated under arid conditions. The sequences identified here are probably comparable in scale to the Phanerozoic cratonic sequences of Sloss ( 1963); hence it is likely that they cannot only be correlated throughout the Wollaston Domain, but possibly with other early Proterozoic successions on the Rae-Hearne Craton (Figure la).

The unconformity is marked by deposition of conglomerate towards the east, and calc-silicate-rich sediments toward the west. Like major unconformities in craton-margin strata of Phanerozoic orogens, this major stratigraphic break probably records migration of a peripheral crustal bulge, formed in response to plate-margin loading by an abducted terrain onto the craton.

These observations also suggest a possible link between the sub-Athabasca uranium deposits associated with basal Wollaston graphitic petites and

44

the Rabbit Lake deposit. If the calc-silicate-rich host rocks at Rabbit Lake belong to the upper sequence, then they probably belong to a TST, as do the graphit ic petites. As discussed above, transgression favours accumulation of organic-rich and phosphatic sediment. It is notable that modem organic-rich phosphorites on the Southwest African Shelf, the Peruvian Shelf, and the Tertiary California Shelf are enriched in uranium (Demaison and Moore, 1980).

A sequence stratigraphic analysis should be applicable to other Precambrian craton margin or platform strata, such as the Hurwitz and Murmac Bay groups (Hartlaub and Ashton, this volume).

8. Acknowledgments Chris Gilboy, Charlie Harper, and Gary Delaney are thanked for their critical reviews of this paper.

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Saskatchewan Geological Survey

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