A Proposed Lithotectonic Domainal Re-classification of the Southeastern Reindeer Zone in Saskatchewan

K.E. Ashton

Ashton, K.E. ( 1999): /\ proposed lithotectonic domainal re-classification of the southcastt:rn Reindeer Zont: in Saskatchewan: in Summary of lnvt:stigations 1999, Volume 1. Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 99-4. 1.

Abstracl

Since the existing lithotectunic domainal classification scheme for the southeastern Reindeer Zone is almost 20 years out-ufdate. the recent literature is marred by numerous inconsistencies and confusion. In this newly proposed classification, the region is sub-divided into: 1) Archean rocks of the Sask Craton exposed in tectonic windows; 2) an expanded Flin Flon Domain, encompassing the Paleoproterozoic vo/cano-p/utonic rocks of the former Hanson lake Block; 3) the Glennie Domain, including the former Scimitar Complex, Ukoop lake Segment, and Nut Bay Belt; 4) the la Range Domain, comprising the Nemeiben Zone, Crew

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lake Belt, and Central Metavolcanic Belt; and 5) the Kisseynew Domain, which includes the jcmner Maclean Lake Belt.

1. Introduction The first attempt to define lithostructural domains in the southeastern part of the exposed Precambrian Shield in Saskatchewan resulted from regional compilations of previous mapping, which led to publication of the 1980 version of the provincial geological map and domainal classification (Figure I; Lewry and Sibbald, 1977; Macdonald and Broughton.

1980). Since that classification

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scheme is now 20 years out-of­date, it is not unreasonable to question whether it still adequately distinguishes domains of distinct lithological and structural (tectonic) character. Such a review is particularly timely in light of the recent completion of the Geological Survey of Canada- Saskatchewan Energy and Mines-Man itoba Energy and Mines collaborative NATMAP Shield Margin Project (Syme et al. , 1998), near completion of the LITHOPROBE Trans-Hudson Orogen Transect, and recent release of a new digital version of the Geological Map of Saskatchewan (Saskatchewan Energy and Mines, 1998).

The 1980 lithotectonic classification followed the

Figure J - 1980 lithotectonic domaina/ clas.fijication for the southeastern Precambrian Shield in Saskatchewan (after Macdonald and Broughton, 1980). Thin contacts denote sub-domain boundaries. Note that the Attitti Block was distinguished as a sub­do111JJin of the Kisseynew Domain but was not formally named unlit the Pelican Narrows and Amisk Lake areas were compiled the following year (Macdonald, 1981).

I: 100 000 scale reconnaissance mapping program of the 1970s, which nearly completed coverage of the province's Shield area outside of the poorly exposed Athabasca Basin . Domains were established based strictly on differences in lithological make­up and/or structural style, and carried no genetic connotations. Domain boundaries were commonly ill defined and many varied in character along strike (e.g. Hanson Lake Block). Only

92 Summary of Investigations /999, Volume I

about IO percent of the Shield has been mapped since 1980, but this recent work has been conducted at the much more detailed scale of l :20 000. Furthermore, it has been focused on areas of h igh mineral potential, which tend to coincide with the tectonically active zones. The resulting determination of numerous fu ndamental geological relationships has been the driving force behind this review.

2. Changes Affecting Oomainal Classification up to 1990

By 1990, several discoveries and changes in our thinking were beginning to produce modified versions of the lithotectonic domainal classification (Figure 2). Archean rocks had been recognized in two tectonic windows in the western G lennie Domain (Chiarenzelli, 1989; Lewry et al. , 1990) and one in the northern Hanson Lake Block (Macdonald. 1974; Bell and Macdonald, 1982; Lewry et al., 1989). All three of these windows are bounded by mylonites indicating major structural discontinuities, which were interpreted

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as plac ing juveni le Paleoprotcrozoic rocks over the Archean material (Lewry et al. , 1990). The lskwatikan Lake and Hunter Bay tectonic windows in the Glennie Domain expose a variety of gne isses and migmatites, which are thought to be of mainly igneous origin (Chiarenzclli , 1989). Archean rocks of the Hanson Lake Block were thought to be restricted to the variably retrogressed Sahli and MacMillan Point charnockitic granites (Lewry et al., 1990), which range from near massive to foliated.

The boundary between the Flin Flon and Kisseynew domains on the 1980 classification (Figure I) was problematic because it was neither lithological nor tectonic. It followed a discontinuous line representing the trans ition from weakly metamorphosed Amisk group and Missi series rocks in the Amisk Lake area into garnet zone and more highly metamorphosed rocks of the Kisseynew gneisses to the north (Byers and Dahlstrom, 1954). Although th is line was intended to mark a metamorphic gradient, it was pointed out that " high grade metamorphic rocks quite indist inguishable from those of the K isseynew" gneisses were also

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locally exposed south of their line.

In the east, the line roughly coincided with a northward change in structural sty le to gentler dips and tighter folds but it was not the sharp structural discontinuity at one time thought to mark this boundary in Manitoba (Harrison, 1951 ). The Annabel Lake Shear Zone, which occurs about 2 km south of the inferred metamorphic transition, was rejected as a tectonic boundary in Saskatchewan because volcanic rocks were abundant farther north (Byers and Dahlstrom, 1954). The idea of using this zone of high strain (under the name Pargas Shear Zone) as a tectonic boundary was later resurrected by Parslow and Gaskarth ( 1988), but was never adopted.

Figur~ 2 - Representative lithotectonic domainal c:las.Iijicatio11 as of about 1990; NZ, Neme,ben Zo_11e, NBB, Nut Bay Belt, MZ, Meraste Zone, SG, Sahli granite; SWSZ, Sturgeon-weir Shear Zone,· mrd black llreas represent Archean tecto11ic windows. Although tire Scimitar Complex was originally intended to form part of the Glennie Domain, it was being included with the Ki~·seynew Domain on many c/assijimtions. Thin contacts de11ote sub-domai11 boundaries.

In the west, Byers and Dahlstrom ( 1954) had demonstrated that the Amisk and Missi rocks, together wi th the regional structure, swung north, and that the Kisscynew gneisses in that region were their more highly metamorphosed equivalents. However, by using d ifferent lithological units for the Kisseynew rocks rather than isograds to infer the metamorphic gradient, they unwitting ly set the stage for the establishment of a domainal boundary based on

Saskatchewan Geological Survey 93

metamorphism in the subsequent domainal classification (Figure I). Although their mapping did not extend as far west as the Sturgeon-weir River, which subsequently became the boundary between the Flin Flon Domain and Hanson Lake Block, their inferred metamorphic line was arbitrarily extended westward by subsequent compilers (Figure I; Macdonald and Broughton, 1980). This area of more highly metamorphosed Amisk and Miss i rocks was distinguished as a sub-domain of the Kisseynew Domain in the 1980 domainal classification (Figure 1; Macdonald and Broughton, 1980), but was not formerly named the Attitti Block until the Pelican Narrows and Amisk Lake areas were compiled the following year (Macdonald, 1981 ).

Re-mapping of this region and subsequent metamorphic studies confirmed that the rocks, the regional structure, and the Annabel Lake Shear Zone all swung northward, whereas the steep metamorphic gradient leveled out and swung southwestward (Ashton et al., 1987; Ashton, 1990, 1992; Ashton and Leclair, I 991 ; Digel et al., 1991 ). Since the continuity with the Flin Flon Domain had been re-affirmed, it was decided to re-establish the domainal boundaries in order to emphasize lithotectonic relationships rather than metamorphic gradients. Thus, the term Attitti Block was abolished, and the rocks of that area were re­assigned to the Flin Flon Domain (Figure 2).

The boundary between the Flin Flon Domain and the Hanson Lake Block had originally been set at the Sturgeon-weir River and defined as either an unconformity or thrust fault (MacQuarrie, 1979). In the 1980 classification, the boundary was interpreted as a shear zone, which was assumed to follow the Sturgeon­weir River from its southern trend, where it is crossed by Highway I 06, to its southeastward swing approaching Amisk Lake. By 1990, it had been shown that the southeast-trending segment of the river followed an older sinistral discontinuity termed the Spruce Rapids Shear Zone, which was displaced by the southern extension of the younger dextral-reverse Sturgeon-weir Shear Zone (Ashton, 1990) . Thus, the small, poorly exposed area east of the Sturgeon-weir Shear Zone and south of the Spruce Rapids Shear Zone was incorporated into the Flin Flon Domain.

The eastern margin of the Glennie Domain had also undergone significant changes since 1980. An eastern apophysis of the northern Glennie Domain had been termed the Scimitar Complex (Figures I and 2) but, due to its apparently distinctive composition of hornblende and biotite paragneisses (e.g . Pearson, 1973), was commonly being included in the Kisseynew Domain (e.g. Saskatchewan Energy and Mines, 1991 , p22 and p3 I). Farther south along the eastern Glennie Domain marg in, recognition of a "straight belt" and strong metamorphic gradients in dominantly psamm itic metasedimentary rocks had apparently justified the distinction of a new domain termed the Ukoop Lake Segment (Saskatchewan Energy and Mines, 1991, p3 l).

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An extensive mapping program in the 1980s (e.g. Thomas, 1993) resulted in subdivision of the La Ronge Domain into the dominantly metasedimentary Crew Lake Belt in the west and Central Metavolcanic Belt in the east (Figure 2). The southwesternmost gneissic to migmatitic part of the Glennie Domain was transferred to the La Ronge Domain, and subdivided into the Nemeiben Zone of dominantly granitoid plutonic rocks, locally rnylonitized gneissic equivalents of the Nut Bay Belt, and intermediate to mafic rocks of the Meraste Zone (Lewry, 1984). Rocks of the Meraste Zone are progressively more mylonitized towards the east, where they grade into the Stanley Shear Zone, which was established as the new boundary between the La Ronge and Glennie domains (Saskatchewan Energy and Mines, 1991 , p22).

The heterogeneous sequence ofpel itic to psamm itic rocks separating the La Ronge and Glennie domains to the north was originally assigned to the Kisseynew gneisses ( e.g. Johnston, 1968) since they appeared to extend continuously into the widespread and compositionally similar Kisseynew gneiss belt to the east. During detailed mapping of the La Ronge Domain, however, workers felt that the sequence represented syn-volcanic sedimentary rocks derived from the west (e.g. Lewry, 1984). Thus, the area was made a separate domain and assigned the name Maclean Lake Belt (e.g. Macdonald and Broughton, 1980). The sedimentary sequence was subdivided into the Maclean Lake Gneisses, comprising mixed psammitic and pelitic rocks, and the overly ing McLennan Group of dominantly pink arkoses, which were viewed as Sickle and/or Missi Group equivalents (Lewry, 1984).

A three-dimensional approach to classifying the southeastern Reindeer Zone in Saskatchewan was introduced about this time by Lewry el al. (1990). It was based on the premise that most of the lithotectonic domains were bounded by a network of mylonite zones, and probably represented thrust nappes. The derived tectonic model drew attention to the idea that the present domainal configuration resulted from plate tectonic activity, which had apparently occurred much as it does in the modern day. It re-opened the problem of the southern La Ronge--G lenn ie dornainal boundary by incorporating the Nerneiben Zone, Nut Bay Belt, and Meraste Zone into1he Wapassini Sheet, which included the northern part of the Glennie Domain. The remaining southern part of the Glennie Domain, which included the Archean tectonic windows, was thought to represent a lower crustal level nappe termed the Cartier Sheet. The Stanley Shear Zone, which had marked the boundary between the Glennie and La Ronge domains in the two-dimensional classification (Mineral Resources of Saskatchewan, 1991 , p22 and p3 I), had been subdivided into the Guncoat Thrust, which was used to mark the western boundary between the Cartier and Wapassini sheets, and the late Stanley Fault. This addressed the observation that rocks of the Nut Bay Belt and Meraste Zone appear continuous with those of the northern Glennie Domain (Lewry and Slimmon, 1985). Although the Nemeiben Zone and Crew Lake Belt were thought to have an arbitrary and transitional

Summary of Investigations 1999, Volume I

boundary, the latter was not included in the Wapassini Sheet, effectively leaving the question of a La Ronge­Glennie dornainal boundary unresolved. While this three-dimensional scheme represented a significant advance in our thinking of the geological history of the Reindeer Zone, not all of the sheet boundaries had been defined and it was not universally adopted.

3. Recent Changes Affecting Domainal Classification

The NATMAP and LITHOPROBE studies of the 1990s generated a renaissance in the way we view the Trans-Hudson Orogen and, in particular, the southeastern part of the Reindeer Zone (e.g. Lucas et al. , 1993). Detailed mapping showed that the Pelican tectonic window south of Pelican Narrows was far more extensive than originally thought (Figure 3) and included abundant pelitic migmatite, ca. 3.0 Ga leucogranodioritic orthogneisses, and a 2.45 Ga multi­phase igneous suite of which the Sahli and MacMillan Point chamockitic granites are an integral part (Ashton

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et al., in press). It is bounded by the 5 km wide Pelican Decollement Zone, which represents the basal sole fault along which the juvenile Paleoproterozoic terrain was thrust southwestwards over the Archean rocks. LITHOPROBE seismic work profiled the Pelican Decollement Zone and showed that the Archean material exposed in the tectonic windows was part of a much more extensive, largely buried body tenned the Sask Craton (Lucas e t al., 1994; Pandit et al. , I 998).

The mixed Paleoproterozoic volcanic, sedimentary, and granodioritic gneisses comprising the hanging wall of the Pelican Decollement Zone are essentially identical to those of the northern Attitti Lake area of the Flin Flon Domain (Ashton e t al., 1993). The previously inferred boundary between the Flin Flon Domain and northern Hanson Lake Block simply represents the eastern extent of mylonitized rocks, which has been overprinted by a late brittle fault. Farther south, the same late fault overprints the Sturgeon-weir Shear Zone, which is rooted in the Pelican Decollement Zone and appears to represent a late splay (Lewry, 1994). Therefore, the main

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lithotectonic break in the Flin Flon- Hanson Lake region is along the Pelican Decollement Zone, which separates the Archean and Paleoproterozoic rock packages, rather than the Sturgeon-weir Shear Zone, which appears to simply offset two broadly correlative segments of the same Paleoproterozoic volcanic-sedimentary­granodioritic belt.

Geochemical and geochronological studies of rocks in the Hanson Lake area are consistent with their being a western extension of the 1.920 to 1.880 Ga (Stem and Lucas, 1994 and references within) volcanic package at Flin Flon. The high proportion of rhyolitic rocks at Hanson Lake suggests that they represent a slightly more evolved part of the arc complex, which is supported by their slightly younger 1.875 to 1.870 Ga ages (Heaman et al., 1993, 1994). Therefore, there appears to be no justification for a distinct Hanson Lake Block. It simply represents a western extension of the Flin Flon Domain (e.g. Maxeiner et al. , in press).

Figure 3 - Proposed new lithotectonic domainal classification for the southeastern Reindeer Zo'!e: NZ, Nemeiben Zone, PDZ, Pelican Decollement Zone; SWSZ, Sturgeon-wetr Shear Zone; and black areas represent Archean tectonic windows. Box with diagonal cross-hatching north of Pelican Narrows denotes the known mylonitic segment of the Glennie-Kisseynew domain al boundary, which is i11/erred to represent re-emergence of the Pelican Di collenrent Zo11e on the northern limb of a regional synfornr; thin dashed lines denote late, regional fold traces.

In the absence of a distinct, continuous structural break, the transition from mixed volcanic, sedimentary, and granodioritic gneisses in the south to dominantly pelitic and psammitic paragneisses in the north has

Saskatchewan Geological Survey 95

been used to mark the northern boundary between the Flin Flon and Kisseynew domains. Weakly defonned rocks along the boundary in the Attitti Lake area, which was in a relative pressure shadow during thrusting along the Pelican Decollement Zone, include amphibolites and calcic pelitic g neisses of the Flin Flon Domain, which g rade into more aluminous equivalents of the Bumtwood Group (Hartlaub el al., 1996). As elsewhere along the boundary, early isoclinal folding resu lted in stratigraphic repetition, but there is no obvious structural break or unconformity, suggesting that the transition may be conformable and record continuous sedimentation from essentially syn-volcanic time (Ansdell and Stem, 1997) throug h to the time of Bumtwood deposition.

Reinterpretation of the hornblende and biotite gneisses comprising the Scimitar Complex as a mixed package of volcanic, sedimentary, and granodioritic gneisses, together with the absence of any obvious structural discontinuities along the inferred western boundary in the Reindeer River area, led to reassignment of the Scimitar Lake area rocks to the Glennie Domain (Ashton el al. , I 996a, 1997). A 1.873 Ga age for a felsic volcanic rock in the southern Scim itar Lake area (Hartlaub et al., 1997a) is well within the age range for volcanism in both the Glennie Domain {Heaman et al., 1992) and Hanson Lake area (Heaman et al., 1993) providing further support for the correlation.

The rock types and proportions constituting the northern Glennie Domain ( including those of the Scimitar Lake area) are remarkably similar to those of the northern Flin Flon Domain. Although the southern boundary between the Scimitar Lake area of the Glennie Domain and the Kisscyncw Domain along the Churchill River is mylonitic, the eastern boundary is a weakly deformed zone of interlayered volcanic rocks and calcic to aluminous pelitic gneisses, similar to that forming the northern Flin Flon- Kisseynew domain boundary north of Attitti Lake (Ashton et al., I 996b; Hartlaub et al. , 1996, I 997b ). The Kisseynew rocks separating the Fl in Flon and G lennie domains in this area lie in the core of a regional synfonn (Figure 3; Lewry et al., 1990), and LITHOPROBE seismic data show that rocks of the Flin Flon Domain extend northward underneath the Kisseynew cover (Lucas et al., 1994). Given their lithological similarity, the lack of a structural discontinuity, and this structural configuration, the simplest interpretation is that the Flin Flon Domain disappears under the southern limb of the synform to re-emerge on the northern limb as the G lennie Domain, inferring that the two are correlative and continuous. This is supported by the presence of the wide, layer-paralle l, mylonite zone spanning the Glennie-Kisseynew domainal boundary along the Churchill River (Figure 3), which has been independently interpreted as a northern extension of the Pelican Decollement Zone, similarly re-emerging on the northern limb of this synform (Ashton et al., I 996b; Hartlaub et al., I 997b ).

Continuity of the Northern Lights volcanic package from the southeastern Glennie Domain eastward across the southern end of the exposed Tabbemor Fault

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furth er supports the Flin Flon-Glennie domain corre lation (Maxeiner et al., in press). It has also been suggested that variably mylon itized and migmatit ic orthogneisses in the hanging wall of the Pelican Decollement Zone west of Pelican Narrows extend continuously underneath rocks of the Kisseynew Domain into the Glennie Domain (Tran et al.. 1996). This study further showed that the psammit ic metascdimentary rocks dominat ing the Ukoop Lake Segment at the eastern marg in of the G lennie Domain unconformably overlie a typical Glennie volcano­plutonic package, re-affirming the area's original inclusion in the Glenn ie Domain . Immediately south. a tonal ite pluton spans the inferred G lcnnie-Kisseynew domain boundary, and is only marginally offset by the late brittle component of deformation along the Tabbernor Fault Zone (Sibbald, 1978; Ashton and Balzer, I 995). The host Bumtwood pelites a lso appear to continue across the boundary, imply ing that rocks of the Kisseynew Domain extend into what had been the southeastern Glenn ie Domain (Figure 3).

The stratigraphic term Flin Flon-Glennie Complex has been ass igned to the volcano-sedimentary-pluton ic package extending continuously from Flin Flon to the Lac La Ronge- Reindeer Lake area in the west (e.g. Ashton et al., 1997), but the Flin Flon and Glennie domains have been retained on the proposed two­dimensional classification due to their physical separation at surface.

The uncovering of a ca. 1.855 Ga unconformity w ithin the Maclean Lake gneisses has shed new light on stratigraphic relationships within the Maclean Lake Belt and on its re lationship to the La Ronge and Kisseynew domains (Maxeiner and Sibbald, 1995). Metasedimentary rocks within an older Assemblage A beneath the unconformity are now considered broadly synchronous with La Ronge Domain volcanism and occupy a simi lar stratigraphic posit ion to syn-volcanic (Heaman el al., 1993; Ansdell and Stem, 1997) parag neisses of the Welsh Lake Assemblage (Reilly, 1993) in the Flin Flon Domain. The younger sedimentary rocks of Assemblage B, which include both pelitic and psarnmit ic rocks of the former Maclean Lake g neisses. as well as the McLennan Group cong lomerates and arkoses, are now considered correlative with the Burntwood and Missi Groups (Maxeiner and Sibbald, 1995). Sedimentation in the Kisseynew Domain also began at about 1.855 Ga, and rapidly evolved into a deposit ional system compris ing a fluvial-alluvial-shallow marine fac ics dominated by conglomerates and arkosic rocks o f the Missi Group and a deeper-water facies represented by aluminous pelites of the Burntwood Group (Syme et al. , 1998). Based on these geochronolog ical and lithologica l s imilarities, and the apparent continuity of rock types across the previously inferred boundary, the MacLean Lake Belt has been incorporated into the Kisseynew Domain.

Since it has been shown that the McLennan Lake Tectonic Zone, w hich was inferred to mark a structural boundary between the La Ronge and Kisseynew (formerly Maclean Lake Belt) domains, is not

Summary of Investigations /999. Volume I

continuous (Yeo. 1996), the lithological change in dominant rock type from volcanic to sedimentary has been used to define the northern part of that domainal boundary.

Although the boundary between the Kisseynew and northwestern Glennie domains is based primarily on the lithological change from dominantly pelitic migmatites to mixed volcanic, sedimentary, and granodioritic gneisses, at least part of it is marked by a structural discontinuity (Harper, 1998). This is consistent with the three-dimensional classification of Lewry et al. ( 1990), who used this boundary to mark the western margin of the Wapassini sheet.

The relationship between the southern La Ronge and Glennie domains continues to be a problem area. There appear to be two possible solutions.

I) There is a tectonic discontinuity separating distinct La Ronge and Glennie domains, which represents a fundamental break along which the Flin Flon­Glennie Complex and rocks of the Kisseynew Domain were accreted to the La Ronge Arc and Hearne Province

2) There is no tectonic discontinuity and rocks of the La Ronge Domain are continuous and correlative with those of the Flin Flon- Glennie Complex .

The problem with the former scenario is that the fundamental break has not been recognized. The degree of deformation increases steadily from the Nemeiben Zone to the mylonites of the Guncoat Thrust, but that discontinuity can be traced continuously into the central Glennie Domain as it is currently defined. Much of the region immediately west of the Guncoat Thrust is mylonit ic, however, so it is possible that another, more fundamental discontinuity is present within the highly strained package.

The second scenario would imply that the La Ronge and Glennie domains together originally formed a single, large, arc complex, which was obliquely accreted to the Hearne province at approximately 1.86 Ga, and then subsequently modified by collision and underplating of the Sask Craton at about 1.84 Ga. Further study is required to resolve this problem. In the meantime, the boundary between the La Ronge and Glennie domains has been set at the approximate contact between the Nemeiben Zone and Nut Bay Belt (Figure 3 ). This is directly along strike of a set of structural discontinuities marking southern truncation of the Kisseynew Domain, Central Metavolcanic Belt, and Crew Lake Belt, which merge on the southeastern margin of the Little Deer Pluton (Lewry and Slimmon, 1985).

As our understanding of the geological relationships and tectonic hi story of this region evolves, further modifications to the domainal classification scheme will be required.

Saskatchewan Geological Survey

4. Acknowledgments

This manuscript is the result o f years of discussions with many colleagues of the Saskatchewan Geological Survey (particularly Torn Sibbald) and others interested in the geology of the Trans-Hudson Orogen . We can attribute much of our understanding of the southeastern port ion of the exposed Precambrian Shie ld in Saskatchewan to the work and insights of John Lewry. Edgar Froese and his concern for "getting things right" and achieving consistency in usage provided much of the stimulus that was necessary to tackle a revision of the nomenclature and domainal class ification scheme. The resulting manuscript was significantly improved following discussions and constructive reviews by Ralf Maxeiner, Edgar Froese, Charlie Harper, and Gary Delaney.

5. References Ansdell, K.M. and Stem, R.A. (1997): SHRIMP

geochronology in the Trans-Hudson Orogen: Detrital zircons in turbiditic and fluvial sed imentary rocks; in Hajnal, Z. and Lewry, J. (eds.), LITHOPROBE Trans-Hudson Orogen Transect, Rep. 62, p 119-125.

Ashton, K.E. ( 1990): Geology of the Snake Rapids area, Flin Flon Domain (parts ofNTS 63L-9 and - IO); in Summary of Investigations 1990, Saskatchewan Geological Survey, Sask. Energy Mines. Misc. Rep. 90-4, p4- I 2.

--~~~ (1 992): Geology of the Mari Lake area, Saskatchewan; Geo!. Surv. Can., Open File 2444, l :50 000 map.

Ashton, K. E. and Balzer, S. ( 1995): Wildnest­Tabbemor Transect: Pelican Lake-Tabbemor Fault area (part of 63M-3); in Summary of Investigations 1995, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 95-4, pl3-22.

Ashton, K.E., Card, C.D., and Harvey, S.E. (1997): Geology of the Mokoman (Knife) Lake-Reindeer River area: The Scimitar Complex and its relationship to the Glennie Domain; in Summary of Investigations 1997, Saskatchewan Geological Survey, Sask. Energy Mines, Misc . Rep. 97-4, p55-64.

Ashton, K.E., Drake, A.J., and Lewry, J .F. (1993): The Wildnest-Tabbemor Transect: Attini-Mirond lakes area (parts ofNTS 63M-1 and -2); in Summary of Investigations 1993, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 93-4, p50-66.

Ashton, K.E., Hartlaub, R.P., Therens, C., and Legault, A. ( l 996b ): The Scimitar Complex-Kisseynew Domain boundary in the Wintego Lake area (part of 63M-IO); in Summary of Investigations 1996,

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Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 96-4, 29-37.

Ashton, K.E., Heaman, L.M., Lewry, J.F. , Hartla ub, R.P., and Shi, R. ( in press): Age and or igin of the Jan Lake Complex: A glimpse at the buried Archean craton of the Trans-Hudson Orogen ; Can. J. Earth Sci.

Ashton, K.E. and Leclair, A.O. ( 199 1): Revision bedrock geological mapping, Wildnest-Attitt i lakes area (parts of NTS 63 M-1 and -2) in Summary of Investigations 1991, Saskatchewan Geolog ical Survey, Sask. Energy Mines, Misc. Rep. 9 1-4, p29-40.

Ashton, K.E., Therens, C., and Legault, A. ( I 996a): Geology of the Scimitar Lake area (part of 63M-15), east-central Scimitar Comp lex; in Summary of Investigations 1996, Saskatchewan Geological Survey, Sask. Energy Mines, M isc. Rep. 96-4, p22-28.

Ashton, K.E., Wilcox, K.H., Wheatley, K.J ., Paul, D., and de Tom be, J. ( 1987): The boundary zone between the Flin Flon Domain, Kisseynew gneisses, and Hanson Lake Block, northern Saskatchewan ; in Summary of Investigations 1987, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 87-4, p 13 1- 134.

Bell, K . and Macdonald, R. ( 1982): Geochrono logical cal ibration of the Precambrian Shie ld in Saskatchewan ; in Summary of Investigations 1982, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 82-4, p 17-22.

Byers, A.R. and Dahls trom , C. D.A. ( 1954): Geology and Mineral Deposits of the Amisk-Wi ldnest Lakes area, Saskatchewan; Sask. Dep. Miner. Resour., Re p. 14, 177p.

Chiarenzelli , J.R. ( 1989): The N istow iak and Guncoat gneisses: Implications for the tectonics o f the G lennie and La Ronge domains, northern Saskatchewan, Canada; unpubl. Ph.D. thesis, Un iv . Kansas, 229p.

Digel, S., Ashton, K.E. , and Wilcox, K.H. ( 1991): Metamorphic P-T investigations in the southern part of Kisseynew and western part of Flin Flon domains; in Summary of Investigat ions 199 1, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 9 1-4 , p41 -46.

Harper, C.T. ( 1998): The La Ronge Domain-Glennie Domain transition: Street Lake area (parts of NTS 640-3 and -6); in Summary of Investigations 1998, Saskatchewan Geologica l Survey, Sask. Energy Mines, Misc. Rep. 98-4 , p66-80.

Harrison , J.M. ( 1951 ): Precambrian correlation and nomenclature, and problems of the Kisseynew gneisses in Manitoba; Geo!. Surv. Can .. Bull. 20, 53p.

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Hartlaub, R.P., Ashton, K.E., and Lewry, J.F. (1996): Geology of the Attitti Block- Kisseynew Domain contact, Belcher Lake area; in Summary of Invest igations 1996, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 96-4, p38-42.

-~,,....--.- ( I 997b ): Geology of the O urom­lskwatam lakes segment of the Churchill River: Bounda ry relations between the Scimitar Complex, Kisseynew Domain, and G lennie Domain; in Summary of Investigations 1997, Saskatchewan Geological Survey, Sask. Energy Mines, M isc. Rep. 97-4, p65-7 1.

Hartlaub, R.P., Heaman, L.M., Ashton, K.E., and Lewry, J.F. (1997a): Prel iminary U-Pb geochronological results from the Pe lican Narrows area; in Hajnal , Z. and Lewry, J . (eds.), LITHOPROBE, T rans-Hudson Orogen Transect, Rep. 62, pl91-196.

Heaman, L.M., Ashton, K.E., Reilly, B.A., Sibba ld, T.1.1., Slimmon, W.L. , and Thomas, D.J. ( 1993): 1992-93 U- Pb geochronological investigations in the Trans-Hudson Orogen, Saskatchewan; in Summary of Investigations 1993, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 93-4, p I 09- 111.

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Tran, H., Lewry, J.F., and Ashton, K.E. ( 1996): The geology of the Medicine Rapids--Grassy Narrows area; in Summary of Investigations 1996, Saskatchewan Geological Survey, Sask . Energy Mines, Misc. Rep. 96-4. p43-50.

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JOO Summary of fnvestigations 1999. Volume 1