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

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 lake Belt, and Central Metavolcanic Belt; and 5) the Kisseynew Domain, which includes the jcmner Since the existing lithotectunic domainal classification Maclean Lake Belt. 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 1. Introduction proposed classification, the region is sub-divided into: 1) Archean rocks ofthe Sask Craton exposed in The first attempt to define lithostructural domains in tectonic windows; 2) an expanded Flin Flon Domain, the southeastern part of th e exposed Precambrian encompassing the Paleoproterozoic vo/cano-p/utonic Shield in Saskatchewan resulted from regional rocks ofth e former Hanson lake Block; 3) the Glennie compilations of previous mapping, which led to Domain, including the former Scimitar Complex, publication of the 1980 version of the provincial Ukoop lake Segment, and Nut Bay Belt; 4) the la geological map and domainal classification (Figure I; Range Domain, comprising the Nemeiben Zone, Crew Lewry and Sibbald, 1977; Macdonald and Broughton. 1980). Since that classification 56°30' scheme is now 20 years out-of date, it is not unreasonable to question whether it still adequately distinguishes domains of distinct lithological and structural (tectonic) character.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-Manitoba 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 + + 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 make up and/or structural style, and 54°30' carried no genetic connotations. Domain boundaries were Figure J - 1980 lithotectonic domaina/ clas.fijication for the southeastern Precambrian commonly ill defined and many Shield in Saskatchewan (after Macdonald and Broughton, 1980). Thin contacts varied in character along strike denote sub-domain boundaries. Note that the Attitti Block was distinguished as a sub (e.g. Hanson Lake Block). Only do111JJin ofthe Kisseynew Domain but was not formally named unlit the Pelican Narrows and Amisk Lake areas were compiled the following year (Macdonald, 1981).

Summary of Investigations /999, Volume I 92 about IO percent of the Shield has been mapped since as plac ing juvenile Paleoprotcrozoic rocks over the 1980, but this recent work has been conducted at the Archean material (Lewry et al. , 1990). The lskwatikan much more detailed scale of l :20 000. Furthermore, it Lake and Hunter Bay tectonic windows in the Glennie has been focused on areas of h igh mineral potential, Domain expose a variety of gneisses and migmatites, which tend to coincide with the tectonically active whi ch are thought to be of mainly igneous origin zones. The resulting determination of numerous (Chiarenzclli, 1989). Archean rocks of the Hanson fu ndamental geological relationships has been the Lake Block were thought to be restricted to the driving force behind this review. variably retrogressed Sahli and MacMillan Point charnockitic granites (Lewry et al., 1990), which range from near massive to fo liated.

2. Changes Affecting Oomainal The boundary between the Flin Flon and Kisseynew Classification up to 1990 domains on the 1980 classification (Figure I) was By 1990, several discoveries and changes in our problematic because it was neither lithological nor thinking were beginning to produce modified versions tectonic. It followed a discontinuous line representing of the lithotectonic domainal classification (Figure 2). the transition from weakly metamorphosed Amisk Archean rocks had been recognized in two tectonic group and Missi series rocks in the Amisk Lake area windows in the western Glennie Domain (Chiarenzelli, into garnet zone and more highly metamorphosed 1989; Lewry et al. , 1990) and one in the northern rocks of the Kisseynew gneisses to the north (Byers Hanson Lake Block (Macdonald. 1974; Bell and and Dahlstrom, 1954). Although this line was intended Macdonald, 1982; Lewry et al., 1989). All three of to mark a metamorphic gradient, it was pointed out that these windows are bounded by mylonites indicating " high grade metamorphic rocks quite indistinguishable major structural discontinuities, which were interpreted from those of the K isseynew" gneisses were also locally exposed south of their line.

In the east, the line roughly coincided with a northward change in structural style to gentler dips and tighter folds but it was not the sharp structural discontinuity at one time thought to mark this boundary in . . KISSEYNEW · . 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.

In th e 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 different 54•30· lithological units for the Kisseynew rocks rather than Figur~ 2 - Representative lithotectonic domainal c:la s.Iijicatio11 as ofabout 1990; NZ, Neme,ben Z o_11e, NBB, Nut Bay Belt, MZ, Meraste Zone, SG, Sahli granite; SWSZ, isograds to infe r the Sturgeon-weir Shear Zone,· mrd black llreas represent Archean tecto11ic windows. metamorphic gradient, they Although tire Scimitar Complex was originally intended to form part of the Glennie unwittingly set the stage for the Domain, it was being included with the Ki~·seynew Domain on many c/assijimtions. establishment of a domainal Thin contacts de11ote sub-domai11 boundaries. boundary based on

Saskatchewan Geological Survey 93 metamorphism in the subsequent domainal An extensive mapping program in the 1980s (e.g. classification (Figure I). Although their mapping did Thomas, 1993) resulted in subdivision of the La Ronge not extend as far west as the Sturgeon-weir River, Domain into the dominantly metasedimentary Crew which subsequently became the boundary between the Lake Belt in the west and Central Metavolcanic Belt in Flin Flon Domain and Hanson Lake Block, their the east (Figure 2). The southwesternmost gneissic to inferred metamorphic line was arbitrarily extended migmatitic part of the Glennie Domain was transferred westward by subsequent compilers (Figure I; to the La Ronge Domain, and subdivided into the Macdonald and Broughton, 1980). This area of more Nemeiben Zone of dominantly granitoid plutonic highly metamorphosed Amisk and Missi rocks was rocks, locally rnylonitized gneissic equivalents of the distinguished as a sub-domain of the Kisseynew Nut Bay Belt, and intermediate to mafic rocks of the Domain in the 1980 domainal classification (Figure 1; Meraste Zone (Lewry, 1984). Rocks of the Meraste Macdonald and Broughton, 1980), but was not Zone are progressively more mylonitized towards the formerly named the Attitti Block until the Pelican east, where they grade into the Stanley Shear Zone, Narrows and Amisk Lake areas were compiled the which was established as the new boundary between following year (Macdonald, 1981 ). the La Ronge and Glennie domains (Saskatchewan Energy and Mines, 1991 , p22). Re-mapping of this region and subsequent metamorphic studies confirmed that the rocks, the The heterogeneous sequence ofpelitic to psammitic regional structure, and the Annabel Lake Shear Zone rocks separating the La Ronge and Glennie domains to all swung northward, whereas the steep metamorphic the north was originally assigned to the Ki sseynew gradient leveled out and swung southwestward (Ashton gneisses ( e.g. Johnston, 1968) since they appeared to et al., 1987; Ashton, 1990, 1992; Ashton and Leclair, extend continuously into the widespread and I 991 ; Digel et al., 1991 ). Since the continuity with the compositionally similar Kisseynew gneiss belt to the Flin Flon Domain had been re-affirmed, it was decided east. During detailed mapping of the La Ronge to re-establish the domainal boundaries in order to Domain, however, workers felt that the sequence emphasize lithotectonic relationships rather than represented syn-volcanic sedimentary rocks derived metamorphic gradients. Thus, the term Attitti Block from the west (e.g. Lewry, 1984). Thus, the area was was abolished, and the rocks of that area were re made a separate domain and assigned the name assigned to the Flin Flon Domain (Figure 2). Maclean Lake Belt (e.g. Macdonald and Broughton, 1980). The sedimentary sequence was subdivided into The boundary between the Flin Flon Domain and the the Maclean Lake Gneisses, comprising mixed Hanson Lake Block had originally been set at the psammitic and pelitic rocks, and the overlying Sturgeon-weir River and defined as either an McLennan Group of dominantly pink arkoses, which unconformity or thrust fault (MacQuarrie, 1979). In the were viewed as Sickle and/or Missi Group equivalents 1980 classification, the boundary was interpreted as a (Lewry, 1984). shear zone, which was assumed to follow the Sturgeon weir River from its southern trend, where it is crossed A three-dimensional approach to classifying the by Highway I 06, to its southeastward swing southeastern Reindeer Zone in Saskatchewan was approaching Amisk Lake. By 1990, it had been shown introduced about this time by Lewry el al. (1990). It that the southeast-trending segment of the river was based on the premise that most of the lithotectonic followed an older sinistral discontinuity termed the domains were bounded by a network of mylonite Spruce Rapids Shear Zone, which was displaced by the zones, and probably represented thrust nappes. The southern extension of the younger dextral-reverse derived tectonic model drew attention to the idea that Sturgeon-weir Shear Zone (Ashton, 1990). Thus, the the present domainal configuration resulted from plate small, poorly exposed area east of the Sturgeon-weir tectonic activity, which had apparently occurred much Shear Zone and south of the Spruce Rapids Shear Zone as it does in the modern day. It re-opened the problem was incorporated into the Flin Flon Domain. of the southern La Ronge--G lenn ie dornainal boundary by incorporating the Nerneiben Zone, Nut Bay Belt, The eastern margin of the Glennie Domain had also and Meraste Zone into1he Wapassini Sheet, which undergone significant changes since 1980. An eastern included the northern part of the Glennie Domain. The apophysis of the northern Glennie Domain had been remaining southern part of the Glennie Domain, which termed the Scimitar Complex (Figures I and 2) but, included the Archean tectonic windows, was thought to due to its apparently distinctive composition of represent a lower crustal level nappe termed the Cartier hornblende and biotite paragneisses (e.g. Pearson, Sheet. The Stanley Shear Zone, which had marked the 1973), was commonly being included in the Kisseynew boundary between the Glennie and La Ronge domains Domain (e.g. Saskatchewan Energy and Mines, 1991 , in the two-dimensional classification (Mineral p22 and p3 I). Farther south along the eastern Glennie Resources of Saskatchewan, 1991 , p22 and p3 I), had Domain margin, recognition of a "straight belt" and been subdivided into the Guncoat Thrust, which was strong metamorphic gradients in dominantly psamm itic used to mark the western boundary between the Cartier metasedimentary rocks had apparently justified the and Wapassini sheets, and the late Stanley Fault. This distinction of a new domain termed the Ukoop Lake addressed the observation that rocks of the Nut Bay Segment (Saskatchewan Energy and Mines, 1991, Belt and Meraste Zone appear continuous with those of p3 l). the northern Glennie Domain (Lewry and Slimmon, 1985). Although the Nemeiben Zone and Crew Lake Belt were thought to have an arbitrary and transitional

94 Summary of Investigations 1999, Volume I boundary, the latter was not included in the Wapassini et al., in press). It is bounded by the 5 km wide Pelican Sheet, effectively leaving the question of a La Ronge Decollement Zone, which represents the basal sole Glennie dornainal boundary unresolved. While this fault along which the juvenile Paleoproterozoic terrain three-dimensional scheme represented a significant was thrust southwestwards over the Archean rocks. advance in our thinking of the geological history of the LITHOPROBE seismic work profiled the Pelican Reindeer Zone, not all of the sheet boundaries had Decollement Zone and showed that the Archean been defined and it was not universally adopted. material exposed in the tectonic windows was part of a much more extensive, largely buried body tenned the Sask Craton (Lucas et al., 1994; Pandit et al. , I 998). 3. Recent Changes Affecting Domainal The mixed Paleoproterozoic volcanic, sedimentary, Classification and granodioritic gneisses comprising the hanging wall The NATMAP and LITHOPROBE studies of the of the Pelican Decollement Zone are essentially 1990s generated a renaissance in the way we view the identical to those of the northern Attitti Lake area of Trans-Hudson Orogen and, in particular, the the Flin Flon Domain (Ashton et al., 1993). The southeastern part of the Reindeer Zone (e.g. Lucas et previously inferred boundary between the Flin Flon al. , 1993). Detailed mapping showed that the Pelican Domain and northern Hanson Lake Block simply tectonic window south of Pelican Narrows was far represents the eastern extent of mylonitized rocks, more extensive than originally thought (Figure 3) and which has been overprinted by a late brittle fault. included abundant pelitic migmatite, ca. 3.0 Ga Farther south, the same late fault overprints the leucogranodioritic orthogneisses, and a 2.45 Ga multi Sturgeon-weir Shear Zone, which is rooted in the phase igneous suite of which the Sahli and MacMillan Pelican Decollement Zone and appears to represent a Point chamockitic granites are an integral part (Ashton late splay (Lewry, 1994). Therefore, the main 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-sedimentary granodioritic 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 ..,,. . ·.,:'". . o:! and refe rences 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). 54°30' In the absence of a distinct, Figure 3 - Proposed new lithotectonic domainal classification for the southeastern continuous structural break, the Reindeer Zo'!e: NZ, Nemeiben Zone, PDZ, Pelican Decollement Zone; SWSZ, transition from mixed volcanic, Sturgeon-wetr Shear Zone; and black areas represent Archean tectonic windows. Box with diagonal cross-hatching north ofPeli can Narrows denotes the known mylonitic sedimentary, and granodioritic segment ofth e Glennie-Kisseynew domain al boundary, which is i11/erred to represent gneisses in the south to re-emergence ofthe Pelican Di collenrent Zo11e on the northern limb ofa regional dominantly pelitic and psammitic synfornr; thin dashed lines denote late, regional fold traces. paragneisses in the north has

Saskatchewan Geological Survey 95 been used to mark the northern boundary between the furth er supports the Flin Flon-Glennie domain Flin Flon and Kisseynew domains. Weakly defonned correlation (Maxeiner et al., in press). It has also been rocks along the boundary in the Attitti Lake area, suggested that variably mylonitized and migmatitic which was in a relative pressure shadow during orthogneisses in the hanging wall of the Pelican thrusting along the Pelican Decollement Zone, include Decollement Zone west of Pelican Narrows extend amphibolites and calcic pelitic gneisses of the Flin Flon continuously underneath rocks of the Kisseynew Domain, which grade into more aluminous equivalents Domain into the Glennie Domain (Tran et al.. 1996). of the Bumtwood Group (Hartlaub el al., 1996). As This study further showed that the psammitic elsewhere along the boundary, early isoclinal folding metascdimentary rocks dominating the Ukoop Lake resu lted in stratigraphic repetition, but there is no Segment at the eastern margin of the G lennie Domain obvious structural break or unconformity, suggesting unconformably overlie a typical Glennie volcano that the transition may be conformable and record plutonic package, re-affirming the area's original continuous sedimentation from essentially syn-volcanic inclusion in the Glennie Domain. Immediately south. a time (Ansdell and Stem, 1997) through to the time of tonalite pluton spans the inferred G lcnnie-Kisseynew Bumtwood deposition. domain boundary, and is only marginally offset by the late brittle component of deformation along the Reinterpretation of the hornblende and biotite gneisses Tabbernor Fault Zone (Sibbald, 1978; Ashton and comprising the Scimitar Complex as a mixed package Balzer, I 995). The host Bumtwood pelites also appear of volcanic, sedimentary, and granodioritic gneisses, to continue across the boundary, implying that rocks of together with the absence of any obvious structural the Kisseynew Domain extend into what had been the di scontinuities along the inferred western boundary in southeastern Glennie Domain (Figure 3). the Reindeer River area, led to reassignment of the Scimitar Lake area rocks to the Glennie Domain The stratigraphic term Flin Flon-Glennie Complex has (Ashton el al. , I 996a, 1997). A 1.873 Ga age for a been assigned to the volcano-sedimentary-plutonic felsic volcanic rock in the southern Scimitar Lake area package extending continuously from Flin Flon to the (Hartlaub et al., 1997a) is well within the age range for Lac La Ronge- Reindeer Lake area in the west (e.g. volcanism in both the Glennie Domain {Heaman et al., Ashton et al., 1997), but the Flin Flon and Glennie 1992) and Hanson Lake area (Heaman et al., 1993) domains have been retained on the proposed two providing further support for the correlation. dimensional classification due to their physical separation at surface. The rock types and proportions constituting the northern Glennie Domain (including those of the The uncovering of a ca. 1.855 Ga unconformity within Scimitar Lake area) are remarkably similar to those of the Maclean Lake gneisses has shed new light on the northern Flin Flon Domain. Although the southern stratigraphic relationships within the Maclean Lake boundary between the Scimitar Lake area of the Belt and on its relationship to the La Ronge and Glennie Domain and the Kisscyncw Domain along the Kisseynew domains (Maxeiner and Sibbald, 1995). Churchill River is mylonitic, the eastern boundary is a Metasedimentary rocks within an older Assemblage A weakly deformed zone of interlayered volcanic rocks beneath the unconformity are now considered broadly and calcic to aluminous pelitic gneisses, similar to that synchronous with La Ronge Domain volcanism and forming the northern Flin Flon- Kisseynew domain occupy a similar stratigraphic posit ion to syn-volcanic boundary north of Attitti Lake (Ashton et al., I 996b; (Heaman el al., 1993; Ansdell and Stem, 1997) Hartlaub et al. , 1996, I 997b). The Kisseynew rocks paragneisses of the Welsh Lake Assemblage (Reilly, separating the Fl in Flon and G lennie domains in this 1993) in the Flin Flon Domain. The younger area lie in the core of a regional synfonn (Figure 3; sedimentary rocks of Assemblage B, which include Lewry et al., 1990), and LITHOPROBE seismic data both pelitic and psarnmit ic rocks of the former show that rocks of the Flin Flon Domain extend Maclean Lake gneisses. as well as the McLennan northward underneath the Kisseynew cover (Lucas et Group conglomerates and arkoses, are now considered al., 1994). Given their lithological similarity, the lack correlative with the Burntwood and Missi Groups of a structural discontinuity, and this structural (Maxeiner and Sibbald, 1995). Sedimentation in the configuration, the simplest interpretation is that the Kisseynew Domain also began at about 1.855 Ga, and Flin Flon Domain disappears under the southern limb rapidly evolved into a deposit ional system comprising of the synform to re-emerge on the northern limb as the a fluvial-alluvial-shallow marine fac ics dominated by G lennie Domain, inferring that the two are correlative conglomerates and arkosic rocks of the Missi Group and continuous. This is supported by the presence of and a deeper-water facies represented by aluminous the wide, layer-parallel, mylonite zone spanning the pelites of the Burntwood Group (Syme et al. , 1998). Glennie-Kisseynew domainal boundary along the Based on these geochronological and lithologica l Churchill River (Figure 3), which has been similarities, and the apparent continuity of rock types independently interpreted as a northern extension of across the previously inferred boundary, the MacLean the Pelican Decollement Zone, similarly re-emerging Lake Belt has been incorporated into the Kisseynew on the northern limb of this synform (Ashton et al., Domain. I 996b; Hartlaub et al., I 997b). Since it has been shown that the McLennan Lake Continuity of the Northern Lights volcanic package Tectonic Zone, w hich was inferred to mark a structural from the southeastern Glennie Domain eastward across boundary between the La Ronge and Kisseynew the southern end of the exposed Tabbemor Fault (formerly Maclean Lake Belt) domains, is not

96 Summary of Investigations /999. Volume I continuous (Yeo. 1996), the lithological change in 4. Acknowledgments dominant rock type from volcanic to sedimentary has been used to define the northern part of that domainal This manuscript is the result of years of discussions boundary. with many colleagues of the Saskatchewan Geological Survey (particularly Torn Sibbald) and others Although the boundary between th e Kisseynew and interested in the geology of the Trans-Hudson Orogen. northwestern Glennie domains is based primarily on We can attribute much of our understanding of the the lithological change from dominantly pelitic southeastern portion of the exposed Precambrian migmatites to mixed volcanic, sedimentary, and Shie ld in Saskatchewan to the work and insights of granodioritic gneisses, at least part of it is marked by a John Lewry. Edgar Froese and his concern for "getting structural discontinuity (Harper, 1998). This is things right" and achieving consistency in usage consistent with the three-dimensional classification of provided much of the stimulus that was necessary to Lewry et al. ( 1990), who used this boundary to mark tackle a revision of the nomenclature and domainal the western margin of the Wapassini sheet. classification scheme. The resulting manuscript was significantly improved following discussions and The relationship between the southern La Ronge and constructive reviews by Ralf Maxeiner, Edgar Froese, Glennie domains continues to be a problem area. There Charlie Harper, and Gary Delaney. appear to be two possible solutions. I) There is a tectonic discontinuity separating distinct 5. References La Ronge and Glennie domains, which represents a fundamental break along which the Flin Flon Ansdell, K.M. and Stem, R.A. (1997): SHRIMP Glennie Complex and rocks of the Kisseynew geochronology in the Trans-Hudson Orogen: Domain were accreted to the La Ronge Arc and Detrital zircons in turbiditic and fluvial Hearne Province sedimentary rocks; in Hajnal, Z. and Lewry, J. (eds.), LITHOPROBE Trans-Hudson Orogen 2) There is no tectonic discontinuity and rocks of the Transect, Rep. 62, p 119-125. La Ronge Domain are continuous and correlative with those of the Flin Flon- Glennie Complex. Ashton, K. E. ( 1990): Geology of the Snake Rapids The problem with the former scenario is that the area, Flin Flon Domain (parts ofNTS 63L-9 and fundamental break has not been recognized. The - IO); in Summary of Investigations 1990, degree of deformation increases steadily from the Saskatchewan Geological Survey, Sask. Energy Nemeiben Zone to the mylonites of the Guncoat Mines. Misc. Rep. 90-4, p4- I 2. Thrust, but that discontinuity can be traced continuously into the central Glennie Domain as it is --~~~ (1 992): Geology of the Mari Lake area, currently defined. Much of the region immediately Saskatchewan; Geo!. Surv. Can., Open File 2444, west of the Guncoat Thrust is mylonitic, however, so it l :50 000 map. is possible that another, more fundamental discontinuity is present within the highly strained Ashton, K. E. and Balzer, S. ( 1995): Wildnest package. Tabbemor Transect: Pelican Lake-Tabbemor Fault area (part of 63M-3); in Summary of The second scenario would imply that the La Ronge Investigations 1995, Saskatchewan Geological and Glennie domains together originally formed a Survey, Sask. Energy Mines, Misc. Rep. 95-4, single, large, arc complex, which was obliquely pl3-22. accreted to the Hearne province at approximately 1.86 Ga, and then subsequently modified by collision Ashton, K.E., Card, C.D., and Harvey, S.E. (1997): and underplating of the Sask Craton at about 1. 84 Ga. Geology of the Mokoman (Knife) Lake-Reindeer Further study is required to resolve this problem. In the River area: The Scimitar Complex and its meantime, the boundary between the La Ronge and relationship to the Glennie Domain; in Summary Glennie domains has been set at the approximate of Investigations 1997, Saskatchewan Geological contact between the Nemeiben Zone and Nut Bay Belt Survey, Sask. Energy Mines, Misc. Rep. 97-4, (Figure 3 ). This is directly along strike of a set of p55-64. structural discontinuities marking southern truncation of the Kisseynew Domain, Central Metavolcanic Belt, Ashton, K.E., Drake, A.J., and Lewry, J .F. (1993): The and Crew Lake Belt, which merge on the southeastern Wildnest-Tabbemor Transect: Attini-Mirond lakes margin of the Little Deer Pluton (Lewry and Slimmon, area (parts ofNTS 63M-1 and -2); in Summary of 1985). Investigations 1993, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 93-4, As our understanding of the geological relationships p50-66. and tectonic hi story of this region evolves, further modifications to the domainal classification scheme Ashton, K.E., Hartlaub, R.P., Therens, C., and Le gault, will be required. A. ( l 996b): The Scimitar Complex-Kisseynew Domain boundary in the Wintego Lake area (part of 63M-IO); in Summary of Investigations 1996,

Saskatchewan Geological Survey 97 Saskatchewan Geological Survey, Sask. Energy Hartlaub, R.P., Ashton, K.E., and Lewry, J.F. (1996): Mines, Misc. Rep. 96-4, 29-37. Geology of the Attitti Block- Ki sseynew Domain contact, Belcher Lake area; in Summary of Ashton, K.E., Heaman, L.M., Lewry, J.F., Hartlaub, Investigations 1996, Saskatchewan Geological R.P., and Shi, R. ( in press): Age and origin of the Survey, Sask. Energy Mines, Misc. Rep. 96-4, Jan Lake Complex: A glimpse at the buried p38-42. Archean craton of the Trans-Hudson Orogen; Can. J. Earth Sci. -~,,....--.- ( I 997b ): Geology of the Ourom lskwatam lakes segment of the Churchill River: Ashton, K.E. and Leclair, A.O. ( 199 1): Revision Boundary relations between the Scimitar bedrock geological mapping, Wildnest-Attitti Complex, Kisseynew Domain, and G lennie lakes area (parts of NTS 63 M-1 and -2) in Domain; in Summary of Investigations 1997, Summary of Investigations 1991, Saskatchewan Saskatchewan Geological Survey, Sask. Energy Geolog ical Survey, Sask. Energy Mines, Misc. Mines, M isc. Rep. 97-4, p65-7 1. Rep. 9 1-4, p29-40. Hartlaub, R.P., Heaman, L.M., Ashton, K.E., and Ashton, K.E., Therens, C., and Legault, A. ( I 996a): Lewry, J.F. (1997a): Preliminary U-Pb Geology of the Scimitar Lake area (part of 63M- geochronological results from the Pelican Narrows 15), east-central Scimitar Comp lex; in Summary area; in Hajnal, Z. and Lewry, J. (eds.), of Investigations 1996, Saskatchewan Geological LITHOPROBE, T rans-Hudson Orogen Transect, Survey, Sask. Energy Mines, M isc. Rep. 96-4, Rep. 62, pl91-196. p22-28. Heaman, L.M., Ashton, K.E., Reilly, B.A., Sibbald, Ashton, K.E., Wilcox, K.H., Wheatley, K.J., Paul, D., T.1.1., Slimmon, W.L., and Thomas, D.J. ( 1993): and de Tom be, J. ( 1987): The boundary zone 1992-93 U- Pb geochronological investi gations in between the Flin Flon Domain, Kisseynew the Trans-Hudson Orogen, Saskatchewan; in gneisses, and Hanson Lake Block, northern Summary of Investigations 1993, Saskatchewan Saskatchewan; in Summary of Investigations Geological Survey, Sask. Energy Mines, Misc. 1987, Saskatchewan Geological Survey, Sask. Rep. 93-4, p I 09-111. Energy Mines, Misc. Rep. 87-4, p 13 1- 134. Heaman, L.M., Kamo, S.L., Ashton, K.E., Reilly, B.A., Bell, K . and Macdonald, R. ( 1982): Geochrono logical Slimmon, W.L., and Thomas, D.J. ( 1992): U-Pb calibration of the Precambrian Shield in geochronological investigati ons in the Trans Saskatchewan; in Summary of Investigations Hudson Orogen, Saskatchewan; in Summary of 1982, Saskatchewan Geological Survey, Sask. investigations 1992, Saskatchewan Geological Energy Mines, Misc. Rep. 82-4, p 17-22. Survey, Sask. Energy Mines, Misc. Rep. 92-4, p 120-123. Byers, A.R. and Dahlstrom, C.D.A. ( 1954): Geology and Mineral Deposits of the Amisk-Wildnest Heaman, L.M., Maxeiner, R.O., and Slimmon, W.L. Lakes area, Saskatchewan; Sask. Dep. Miner. ( 1994): 1993-94 U-Pb geochrono logical Resour., Rep. 14, 177p. investigations in the Trans-Hudson Orogen, Saskatchewan; in Summary of Investigations Chiarenzelli, J.R. ( 1989): The N istowiak and Guncoat I 994, Saskatchewan Geological Survey, Sask. gneisses: Implications for the tectonics o f the Energy Mines, Misc. Rep. 94-4, p96-99. G lennie and La Ronge domains, northern Saskatchewan, Canada; unpubl. Ph.D. thesis, Johnston, W.G .Q. (1968): The Geology of the Kelly Univ . Kansas, 229p. Lake Area; Sask. Dep. Miner. Resour., Rep. I 06, 64p. Digel, S., Ashton, K.E. , and Wilcox, K.H. ( 1991): Metamorphic P-T investigations in the southern Lewry, J.F. ( 1984): Bedrock compilation, Lac La part of Kisseynew and western part of Flin Flon Ronge and Wapawekka areas (NTS 73P/731); in domains; in Summary of In vestigations 1991, Summary of Investigations 1984, Saskatchewan Saskatchewan Geological Survey, Sask. Energy Geolog ical Survey, Sask. Energy Mines, Misc. Mines, Misc. Rep. 9 1-4, p41 -46. Rep. 84-4, p34-4 l .

Harper, C.T. ( 1998): The La Ronge Domain-Glennie ( 1994): Rooting of the Sturgeon-weir Domain transition: Street Lake area (parts of NTS ~ear Zone in the Pelican Slide, Gooding Lake 640-3 and -6); in Summary of Investigations Sturgeon-weir River area; in Summary of 1998, Saskatchewan Geological Survey, Sask. Investigations 1994, Saskatchewan Geological Energy Mines, Misc. Rep. 98-4, p66-80. Survey, Sask. Energy Mines, Misc. Rep. 94-4, p 132-1 36. Harrison, J.M. ( 1951 ): Precambrian correlation and nomenclature, and problems of the Kisseynew Lewry, J.F., Macdonald, R. , and Stauffer. M.R. ( 1989): gneisses in Manitoba; Geo!. Surv. Can .. Bull. 20, The development of highly strained rocks in the 53p. Pelican Window during hig h-grade metamorphism

98 Summary of Investigations I 999. Volume I and pervasive anatexis; in Summary of Survey, Sask. Energy Mines, Misc. Rep. 95-4, Investigations 1989, Saskatchewan Geological p79-85. Survey, Sask. Energy Mines, Misc. Rep. 89-4, p58-65. Maxeiner, R.O., Sibbald, T.l.I., Slimmon, W.L., Heaman, L.M., and Watters, B.R. (in press): Lewry, J.F. and Sibbald, T.1.1. ( 1977): Variation in Lithogeochemistry of volcano-plutonic lithology and tectonometamorphic relationships in assemblages of the southern Hanson Lake Block the Precambrian basement of northern and southeastern Glennie Domain , Trans-Hudson Saskatchewan; Can. J. Earth Sci., v14, pl453- Orogen: Evidence for a single island arc complex; 1467. Can. J. Earth Sci.

Lewry, J.F. and Slimmon, W.L. (1985): Compilation Pandit, B.I., Hajnal, Z., Stauffer, M.R., Lewry, J.F., Bedrock Geology, Lac La Ronge, NTS Area and Ashton, K.E. ( 1998): New seismic images of 73 P/731; Sask. Energy Mines, Rep. 225, I :250 000 the crust in the central Trans-Hudson Orogen of scale map w ith marginal notes. Saskatchewan; Tectonophysics, v290, p2 I l-2 I 9.

Lewry, J.F. , Thomas, D.J., Macdonald, R., and Parslow, G.R. and Gaskarth, J.W. (1988): Proterozoic Chiarenzelli, J. (1990): Structural relations in rocks of east-central Saskatchewan: Geochemistry, accreted terranes of the Trans-Hudson Orogen, structure and mineralization controls; in Summary Saskatchewan: Telescoping in a collisional of Investigations 1988, Saskatchewan Geological regime?; in Lewry, J.F. and Stauffer, M.R., (eds.), Survey, Sask. Energy Mines, Misc. Rep. 88-4, The Early Proterozoic Trans-Hudson Orogen of pl27-1 39. North America, Geo!. Assoc. Can., Spec. Pap. 37, p75-94. Pearson, D.E. ( 1973): The Geology of the Scimitar Lake Area (east halt), Saskatchewan; Sask. Dep. Lucas, S.B. , Green, A., Hajnal, Z., White, D., Lewry, Miner. Resour., Rep. 156, I 7p. 1., Ashton, K., Weber, W., and Clowes, R. (1993): Deep seismic profile across a Proterozoic collision Reilly, B.A. ( 1993 ): Revision bedrock geological zone: Surprises at depth; Nature, v363, p339-342. mapping of the northwest Amisk Lake area (parts ofNTS 63L-9 and -16); in Summary of Lucas, S. B., White, D., Hajnal, Z., Lewry, J., Green, Investigations 1993, Saskatchewan Geological A., Clowes, R., Zwanzig, H., Ashton, K., Survey, Sask. Energy Mines, Misc. Rep. 93-4, Schledewitz, D., Stauffer, M., Norman, A., p1 2-20. Williams, P.F., and Spence, G. (1994): Three dimensional collisional structure of the Trans Saskatchewan Energy and Mines (1991): Mineral Hudson Orogen, Canada; Tectonophysics, v232, resources of Saskatchewan, Sask. Energy Mines, pl6 1-1 78. Misc. Rep. 91-5, 76p.

Macdonald, R. ( 1974): Pelican Narrows (West) area, _ ___ ( 1998): Geological map of Saskatchewan, reconnaissance geological survey of 63-M-2(W); version 1.0, digital map and datasets. in Summary Report of Field lnvestigations 1974, Saskatchewan Geological Survey, Sask. Dep. Sibbald, T.l.I. ( 1978): Geology of the Sandy Narrows Miner. Resour., p30-37. (East) Area, Saskatchewan (NTS area 63M-3E); Sask. Dep. Miner. Resour., Rep. 170, 49p. Macdonald, R. ( 198 1) : Compilation bedrock geology: Pelican Narrows and Amisk Lake areas (NTS Stern, R.A . and Lucas, S.B. (1994): U-Pb zircon age 63M, 6JL and part 63N and 63K); in Summary of constraints on the early tectonic history of the Flin In vestigations 1981, Saskatchewan Geological Flon accretionary collage, Saskatchewan; in Survey, Sask. Dept. Miner. Resour., Misc. Rep. Radiogenic A ge and Isotopic Studies: Report 8; 81-4, p l 6-23. Geol. Surv. Can., Current Research 1994-F, p75- 86. Macdonald, R. and Broughton, P. ( 1980): Geological map of Saskatchewan, provisional edition, 1980, Syme, E.C. , Lucas, S.B., Zwanzig, H.V., Bailes, A.H., Sask. Miner. Resour., I: I 000 000 scale. Ashton, K.E., and Haid!, F.M. ( 1998): Geology, NA TMAP Shield Margin Project area of Flin Flon MacQuarrie, R.R. ( 1979): Geological re-investigation Belt, Manitoba/Saskatchewan accompanying notes mapping, Birch Portage south, NTS area (63L- to Geo!. Surv. Can. Map l 968A, Manit. Energy l 5S); in Summary of Investigations 1979, Mines Map A-98-2, Sask. Energy Mines Map Saskatchewan Geological Survey, Sask. Dep. 258A. Miner. Resour. , Misc. Rep. 79-10, p29-38. Thomas, D.J. (1993): Geology of the Star Lake-Otter Maxeiner, R.O. and Sibbald, T.l.l. ( 1995): Lake Portion of the Central Metavolcanic Belt, La Controversial rocks in the Hebden-MacKay lakes Ronge Domain; Sask. Energy Mines, Rep. 236, area, southern La Ronge Domain; in Summary of 132p. Investigations 1995, Saskatchewan Geological

Saskatchewan Geological Survey 99 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.

Yeo, G.M. (1996): Geologic investigations in the Scriver Lake area, La Ronge Domain (NTS 73 P l 6-NE); in Summary of Investigations 1996, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 96-4, p79-9 l.

JOO Summary of fn vestigations 1999. Volume 1