Slave Craton and Wopmay Orogen, NW Canada

Canadian Journal of Earth Sciences

Parentage of Archean basement within a Paleoproterozoic orogen and implications for on-craton diamond preservation: Slave craton and Wopmay orogen, NW Canada

Journal: Canadian Journal of Earth Sciences

Manuscript ID cjes-2016-0059.R1

Manuscript Type: Article

Date Submitted by the Author: 01-Sep-2016

Complete List of Authors: Ootes, Luke; Northwest Territories Geological Survey; British Columbia Geological DraftSurvey; Arctic Institute of North America Jackson, Valerie; Northwest Territories Geological Survey; Arctic Institute of North America; 3126 Westridge Pl Davis, William; Geological Survey of Canada Bennett, Venessa; Geomantia Consulting Smar, Leanne; Desert Star Resources Cousens, Brian; Carleton University, Earth Sciences

Wopmay orogen, Archean basement, rift-related thermal weakening, Slave Keyword: craton, diamond preservation

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Parentage of Archean basement within a Paleoproterozoic orogen and implications for oncraton diamond preservation: Slave craton and Wopmay orogen, NW Canada

Luke Ootes* and Valerie A. Jackson^ Northwest Territories Geological Survey, Box 1320, Yellowknife, NT, Canada X1A 2L9 and Arctic Institute of North America, University of Calgary, 2500 University Drive NW, Calgary, AB, T2N 1N4

^current address: * British Columbia Geological Survey, Box 9333 Stn Prov Govt, Victoria, BC, Canada V8W 9N3 corresponding author: [email protected] Ph. 2503872021

^3126 Westridge Pl, Victoria, BC, Canada V9E 1C8 [email protected]

William J. Davis Draft Geological Survey of Canada, 601 Booth Street, Ottawa, ON, Canada K1A 0E8 [email protected]

Venessa Bennett Geomantia Consulting, 33 Roundel Road, Whitehorse, YT, Canada Y1A 3H4 [email protected]

Leanne Smar Desert Star Resources, 7171030 West Georgia St,, Vancouver, BC, Canada V6E 2Y3 [email protected]

Brian L. Cousens Department of Earth Sciences, Carleton University, 1125 Colonel By Drive, Ottawa, ON, Canada K1S 5B6 [email protected]

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Abstract The Wopmay orogen is a Paleoproterozoic accretionary belt preserved to the west of the Archean Slave craton, NW Canada. Reworked Archean crystalline basement occurs in the orogen and new bedrock mapping, UPb geochronology, and SmNd isotopic data further substantiate a Slave craton parentage for this basement. Detrital zircon results from unconformably overlying Paleoproterozoic supracrustal rocks also support a Slave craton provenance. Rifting of the Slave margin began at ca. 2.02 Ga with a second rift phase constrained between ca. 1.92 and 1.89 Ga, resulting in thermal weakening of the Archean basement and allowing subsequent penetrative deformation during the Calderian orogeny (ca. 1.88 to 1.85 Ga). The boundary between the western Slave craton and the reworked Archean basement in the southern Wopmay orogen is interpreted as the rifted cratonic margin, which later acted as a rigid backstop during compressional deformation. Ageisotopic characteristics of plutonic phases track the extent and evolution of these processes that left penetratively deformed Archean basement, Paleoproterozoic cover,Draft and plutons in the west, and ‘rigid’ Archean Slave craton to the east. Diamondbearing kimberlite occurs across the central and eastern parts of the Slave craton, but kimberlite (diamondbearing or not) has not been documented west of ~114 ⁰W. It is proposed that, while the crust of the western Slave craton escaped thermal weakening, the mantle did not and was moved out of the diamond stability field. The Paleoproterozoic extension convergence cycle preserved in the Wopmay orogen provides a reasonable explanation as to why the western Slave craton appears to be diamondsterile.

Keywords: Wopmay orogen, internal metamorphic zone, Archean basement, riftrelated thermal weakening, Slave craton, diamond preservation

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INTRODUCTION The Slave craton, in northwest Canada, is a crustal block that formed and ‘cratonized’ during the Archean eon (Kusky 1989; Bleeker 2002; Davis et al. 2003a; Helmstaedt 2009; Heaman and Pearson 2010). Immediately west of the Slave craton is the Wopmay orogen, which contains Archean basement exposures and Paleoproterozoic supracrustal and plutonic rocks (St Onge et al. 1983, 1991; Hoffman 1984; King 1987; Hildebrand et al. 1991, 2010; Jackson 2008; Hoffman et al. 2011; Jackson and Ootes 2012; Jackson et al. 2013). Collectively, these rocks underwent penetrative ductile deformation and associated metamorphism during the Paleoproterozoic (King 1987; StOnge et al. 1991; Jackson et al. 2013). Two competing interpretations have been proposed for the parentage of the deformed Archean basement in Wopmay orogen: 1) it originated as part of the Slave craton, but underwent reworking in the Proterozoic (Jackson et al. 2013), or 2) it was part of an exotic microcontinent (Hottah terrane) and structurally emplaced over the western Slave craton and its margin, and is now preserved as a klippe (Hildebrand et al. 2010). Draft In this contribution we present results from bedrock mapping, UPb zircon geochronology, and wholerock Nd isotopic fingerprinting of the Archean basement exposures in the Wopmay orogen. We also present detrital zircon UPb data from metasedimentary rocks that unconformably overly this Archean basement. The integration of these datasets further demonstrates that the Archean basement exposures and overlying sedimentary rocks have a Slave craton parentage/provenance and provide a revised understanding of the architecture of the rifted western cratonic margin. In turn, this has implications for the Slave craton’s lithospheric evolution and provides insights into the diamond fertility of its western region. For example, diamondbearing kimberlites are prevalent across the central and eastern parts of the Slave craton, but after intense exploration efforts during the past two decades, no oncraton kimberlite has been discovered west of 114 ⁰W, or within the eastern parts of the Wopmay orogen. In northern Canada, diamondbearing kimberlites have generally been discovered using dispersed diamondindicator minerals in glacial till. Have no kimberlites been discovered because they do not contain diamonds and therefore the glacially dispersed till does not contain the appropriate diamond indicator minerals? Oncraton studies have yet to provide a resolution of this paradox; however, the Archean basement in the adjacent Paleoproterozoic orogenic belt may contain the clues for resolving western Slave craton diamond enigma.

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GEOLOGICAL BACKGROUND Slave Craton The Slave craton (Fig. 1) is a 4.02 to 2.55 Ga composite cratonic block (Kusky 1989; Bleeker 2002; Davis et al. 2003a, b; Snyder 2008; Helmstaedt 2009; Heaman and Pearson 2010). The westcentral Slave craton contains bedrock older than ca. 2.85 Ga, preserved as gneissic basement complexes and a late Mesoarchean supracrustal cover sequence (Bleeker et al. 1999, 2000; Sircombe et al. 2001; Bleeker 2002; Ketchum et al. 2004; Reimink et al. 2014). Stratigraphically above the basement and cover are Neoarchean volcanic belts (>2.73 Ga to ca. 2.66 Ga; e.g., Bleeker 2002) and greywackemudstone successions (ca. 2.66 to 2.62 Ga; Ootes et al. 2009; Haugaard et al. 2016), as well as late polymictic conglomerates and sandstones (<2.6 Ga; Corcoran and Mueller 2002). The western Slave craton is dominated by ca. 2630 to 2580 Ma plutonic rocks (van Breemen et al. 1992; Davis and BleekerDraft 1999; Bennett et al. 2005), and the youngest identified is the Stagg granite, dated at 2565.4 ± 4.1 Ma (Bleeker et al. 2007). Metamorphic grade in the western Slave craton is variable, but generally characterized by hightemperature, lowpressure, greenschist to granulitefacies assemblages preserved in both volcanic and sedimentary rocks and spatially associated with granitic intrusions (Davis and Bleeker 1999; Pehrsson et al. 2000; Bennett et al. 2005; Ootes et al. 2005). Upperamphibolite to granulitefacies assemblages are locally wellpreserved and metamorphism occurred between ca. 2600 and 2580 Ma (e.g., Pehrsson et al. 2000; Bennett et al. 2005; Ootes et al. 2005; Jackson et al. 2006). Metamorphism in the deep crust continued to ca. 2550 Ma, as recorded by lower crustal xenoliths recovered from kimberlites (Davis et al. 2003a). The timing of penetrative ductile deformation in the Slave craton is best documented in the Duncan Lake Group greywackemudstone successions, where

D1D2 occurred between ca. 2650 and 2590 Ma, with a younger D 3 overprint (Bleeker and BeaumontSmith 1995; Davis and Bleeker 1999; Bleeker 2002; Ootes et al. 2005). The Mesoarchean and older basement has a more complicated history of deformation (e.g., Bleeker et al. 1999; Ketchum et al. 2004), whereas plutonic rocks younger than ca. 2590 Ma do not contain penetrative deformation fabrics (Pehrsson 2002; Bennett et al. 2005; Jackson et al. 2006). The Slave craton does not contain postArchean ductile deformationrelated fabrics, nor metamorphic assemblages, with the possible exception of its eastern boundary with the Thelon orogen

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(Culshaw 1991). The Slave craton was, however, subjected to brittle Paleoproterozoic compressional and extensional deformation preserved as faults and mafic dyke swarms (Kusky et al. 1993; Pehrsson 2002; Jackson et al. 2006; Buchan and Ernst 2013; Buchan et al. 2016). The Slave craton hosts numerous diamondiferous kimberlite pipes and dykes, including the Diavik and Ekati mines, the forthcoming Gahcho Kué mine, and the pastproducing Snap Lake and Jericho mines. These kimberlites intruded into the craton during the Phanerozoic (Heaman et al. 2004) and tapped and transported subcontinental lithospheric mantle, and associated diamonds, that had previously formed in the Archean and Proterozoic (Pearson and Wittig 2008; Heaman and Pearson 2010; Kopylova et al. 2016). These diamondiferous kimberlites are almost entirely within the central and eastern part of the craton, and at this time no oncraton kimberlite has been discovered west of the gneissic basement, west of about 114 ⁰W (Fig. 1A). The western margin includes areas known to contain Mesoarchean and older basement, a key ingredient in diamond preservation in the central and eastern part of the craton (e.g., Snyder et al. 2014), yet remains aDraft kimberlite and diamondfree zone.

Wopmay orogen The Wopmay orogen occurs to the west of the Slave craton (Fig. 1). The orogen records a history of initial rifting of the western Slave craton between ca. 2.05 to 2.01 Ga, passive margin sedimentation at ca. 1.97 Ga, and active margin sedimentation at ca. 1.88 Ga (Coronation basin; Bowring and Grotzinger 1992; Hildebrand et al. 2010; Hoffman et al. 2011). The orogen is bisected by the northstriking Wopmay fault zone (Fig. 1). West of the fault zone are the Hottah terrane and overlying Great Bear magmatic zone (Hildebrand et al. 1987, 2010; Gandhi et al. 2001; Davis et al. 2015; Ootes et al. 2015). The area immediately east of the fault zone is the subject of this paper. It was originally interpreted as metamorphosed parts of the Coronation margin, and referred to as the metamorphic internal zone of the Wopmay orogen (Fig. 1B; e.g., Hoffman 1984; King 1987). This zone was subsequently reinterpreted as a thrust sheet of the Hottah terrane (Figs. 1C, 2, and 3A; Hildebrand et al. 1990, 1991, 2010). The Asiak fold and thrust belt, which occurs in the northeastern part of the Wopmay orogen (north of 65 ⁰30’N), includes sedimentary and minor volcanic rocks of the initial rift sequence of the Melville Group (ca. 2014 Ma), the passive margin stratigraphy of the Epworth Group (ca. 1970 Ma), and the foredeep sedimentary rocks of the Recluse Group (ca. 1882 Ma), all of which were deposited on

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6 the Slave craton (Fig. 3A; Hoffman 1984, 1996; Bowring and Grotzinger 1992; Hoffman et al. 2011). In our following overview and discussion, we rely heavily on bedrock geology maps, as all interpretations are presumably built on the mapping results. The key bedrock geology maps regarding the study area in question are by Hoffman (1984, 1996), Frith (1986), StOnge et al. (1991), Pehrsson (2002), Jackson et al. (2006), Jackson (2008), Jackson and Ootes (2012).

Hottah Terrane and Great Bear magmatic zone The Hottah terrane is preserved west of the Wopmay fault zone, although some rock units east of this fault have also been interpreted as part of this terrane (Figs. 1C, 2, and 3A; Hildebrand et al. 1990, 1991, 2010; Hoffman and Hall 1993; Hildebrand 2011; Hoffman et al. 2011). The oldest exposed bedrock in the terrane is composed of metasedimentary and metavolcanic rocks that were deposited at ca. 1950 Ma (Holly Lake metamorphic complex) and these were intruded by relatively juvenile plutonic phases between ca. 1930 and 1910 Ma (Hottah plutonic complex; Fig. 3B; BowringDraft 1984; Davis et al. 2015; Ootes et al. 2015). The plutonic rocks and metamorphic rocks are unconformably overlain by the Bell Island Bay Group, which consists of basal Beaverlodge Lake sandstone and subaerial rhyolite and lesser basalt of the Zebulon Formation, overlain by quartz arenite and mudstone of the Conjuror Bay Formation, and capped by pillow basalt and lesser rhyodacite of the Bloom Basalts that were emplaced between ca. 1906 and 1893 Ma (Fig. 3B; Hildebrand et al. 1983; Reichenbach 1991; Ootes et al. 2015). The Hottah terrane’s detrital zircon record indicates a dominant ca. 2.01.97 Ga source, with relic Orisirian, Rhyacian, Siderian, and scant Neoarchean zircons (Davis et al. 2015). Whereas the δ18 O and LuHf isotope signatures of these detrital zircons indicate that the evolution of the Hottah terrane started in the Neoarchean (Davis et al. 2015), there are neither bedrock exposures nor direct isotopic signatures to support that Archean basement underlies it (Fig. 3B; Bowring and Podosek 1989; Ootes et al. 2015). The Hottah terrane was extensively intruded and unconformably overlain by ca. 1875 to 1850 Ma Great Bear magmatic zone igneous rocks (Bowring 1984; Gandhi et al. 2001; Ootes et al. 2015). These elements do not contain Archean crust, but a magnetotelluric transect indicates that mantle of the Slave craton continues under these at depth (Spratt et al. 2009).

Slave craton to Wopmay fault zone

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In the northern Wopmay orogen (north of 65 ⁰N), parts of the area east of the Wopmay fault zone and west of the Slave craton are composed of Coronation margin rocks underlain by Archean basement. Two ‘styles’ of Archean basement are preserved, one that is contiguous with the Slave craton and not penetratively deformed in the Proterozoic (e.g., the Acasta area), and one that is isolated from the Slave craton and was penetratively deformed in the Proterozoic (e.g., Bent gneiss; Figs. 1 and 2; Hoffman 1984, 1986; StOnge et al. 1991). Archean basement that is correlated with the Slave craton is unconformably overlain by rocks assigned to the Odjick Formation of the Epworth Group (Hoffman 1984, 1996; StOnge et al. 1991). Archean basement of uncertain parentage is overlain by sedimentary rocks that have been assigned to the Akaitcho Group and Grant Subgroup (e.g., Easton 1980, 1981a, b; Hoffman 1984; King 1987; King et al. 1987; StOnge and King 1986, 1987; StOnge et al. 1991). Rhyolites and sills within the Akaitcho Group and Grant Subgroup have been dated at ca. 1.9 Ga (Bowring 1984), the Zephyr arkose has yielded a maximum deposition age of 1894.7 ± 0.9 Ma (Hoffman et al. 2011), and a rhyodacite dated at 1892.9 ± 1.4 MaDraft (Fig. 3B; Ootes et al. 2015). The Grant Subgroup and Akaitcho Group volcanic rocks have Nd isotope compositions that indicate these rocks are relatively juvenile ( εNd T = 0.3 to 2.3; Bowring and Podosek 1989; Ootes et al. 2015). King et al. (1987) describe two locations and Hildebrand et al. (1991) one location where the Akaitcho Group unconformably overlies the Archean basement. However, those supracrustal rocks, along with the underlying Archean basement have been variably deformed and metamorphosed, complicating stratigraphic interpretations and reconstructions (Easton 1980, 1981a, b; Bowring 1984; Hoffman 1984, 1996; King 1987; King et al. 1987; StOnge and King 1986, 1987; St Onge et al. 1991). The Hepburn intrusive suite was emplaced into, and deformed with the Akaitcho Group and Epworth Group. The plutons are generally cited as ca. 1885 Ma, a mean of ages ranging from >1890 Ma to ca. 1865 Ma (Bowring 1984; Hildebrand et al. 2010) and their Nd and Pb isotopic values indicate they neither melted from, nor were significantly contaminated by Archean basement (Bowring and Podosek 1989; Housh et al. 1989). The Hepburn intrusive suite was originally interpreted to have been emplaced into a closing ensialic backarc basin (Hoffman et al. 1980; Lalonde 1989), but later interpreted as magmatism within a forearc environment (Hildebrand et al. 2010). Hepburn intrusive suite plutons have not been found south of about 65 ⁰20’N (StOnge et al. 1991; Jackson et al. 2013). The Bishop intrusive suite plutons were emplaced between ca. 1.86 to 1.85 Ga and were not subjected to penetrative deformation

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(Bowring 1984; StOnge et al. 1991). Their isotopic values (Nd, Pb) indicate interaction with, or partial derivation from Neoarchean basement (Bowring 1984; Lalonde 1989; Bowring and Podosek 1989; Housh et al. 1989). In the southern Wopmay orogen (south of 65⁰N), in the area between Wopmay fault zone and the contiguous Slave craton, the bedrock exposure comprises >35% Archean basement, mostly Neoarchean in age (ca. 2.58 Ga; Figs. 3B and 4; Jackson 2008; Jackson and Ootes 2012; Bennett et al. 2012; Jackson et al. 2013). This basement is composed of strongly deformed to gneissic rocks with plutonic and metasedimentary protoliths, as well as resorbed mafic dykes, presumably of Paleoproterozoic age (StOnge et al. 1991; Jackson 2008; Jackson and Ootes 2012; Bennett et al. 2012; Jackson et al. 2013). The penetrative deformation fabrics in these basement rocks are manifested as mineraldefined foliations and lineations, gneissic layering (compositional and injection layering), folds and boudinage (e.g., Fyson and Jackson 2008; Jackson 2008; Jackson and Ootes 2012; Jackson et al. 2013). These basement occurrences are in many places unconformably overlain byDraft Paleoproterozoic marble/calcsilicate, quartz arenite, rusty (pyritic) psammite, pelite, and amphibolite (Fig. 3B; Jackson 2008; Jackson and Ootes 2012; Jackson et al. 2013). The supracrustal rocks contain folds and mineraldefined deformation fabrics and are metamorphosed (Fyson and Jackson 2008; Jackson 2008; Jackson and Ootes 2012; Smar 2015), but in many locations compositional characteristics preclude widespread porphyroblast development. Local porphyroblast development and qualitative and quantitative P T modeling indicate low to moderatepressure greenschist to upper amphibolite, and locally granulite facies conditions (StOnge and King 1986; StOnge et al. 1991; Jackson 2008; Jackson and Ootes 2012; Jackson et al. 2013; Smar 2015). Jackson et al. (2013) were uncertain about which stratigraphic assignment was correct for these supracrustal rocks and simply referred to them as the Coronation margin sedimentary sequence (Fig. 4; Jackson 2008). The Archean basement and its cover were intruded by rare granitic sills at ca. 1877 Ma, granodiorite plutons at ca. 1867 Ma (Zinto intrusive suite), and voluminous coarsely Kfeldspar phenocrystic granitic plutons at ca. 1858 to 1850 Ma, which are equivalent to the Bishop intrusive suite to the north (Jackson et al. 2013). Both the ca. 1877 and 1867 Ma plutons contain penetrative deformation fabrics in the form of mineraldefined foliations and the older granitic sills are folded with the host sedimentary rocks (Jackson and Ootes 2012; Jackson et al. 2013; Smar 2015). The ca. 1855 Ma plutons were not deformed in a ductile fashion. As a result, the timing of deformation and

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metamorphism of the metasedimentary rocks is bracketed by the plutonic phases to have occurred between ca. 1877 and 1860 Ma.

Tectonic Models The Archean basement rocks and overlying Akaitcho Group and Grant Subgroup (ca. 1.9 Ga) within the metamorphic internal zone of the Wopmay orogen were interpreted as a rift sequence, and penetratively deformed during the Paleoproterozoic, whereas the contiguous Slave craton was not (Fig. 1B; Easton 1980, 1981a, b; Hoffman 1984; King 1987; King et al. 1987; St Onge and King 1986, 1987; Lalonde 1989). The Akaitcho Group was considered as the initial rift in the Wopmay orogen (Easton 1981a; Hoffman and Bowring 1984). Subsequent UPb zircon dating of ash beds in the Kilohigok basin, thought to be correlative to the Epworth Group passive margin sedimentary rocks in the Coronation basin, indicated deposition at ca. 1.97 Ga (Bowring and Grotzinger 1992). Consequently, Bowring and Grotzinger (1992) concluded that the Akaitcho Group could not representDraft the initial rift sequence. This has been substantiated by UPb zircon dating of a felsic ash bed in the Melville Group, indicating this tuff was deposited at ca. 2014 Ma, and interpreted as the rift to drift marker in the orogen (Hoffman et al. 2011). The fact that the Akaitcho Group was not the initial rift in the Wopmay orogen, led in part to the reinterpretation that these supracrustal rocks, any underlying Archean basement, and younger Hepburn intrusive suite, were part of the exotic Hottah terrane, now preserved as a klippe (Turmoil klippe) on the western Slave craton margin (Figs. 1C and 2; Hildebrand et al. 1990, 1991, 2010; Hoffman and Hall 1993; Hildebrand 2011; Hoffman et al. 2011). These interpretations were derived mostly from work north of 65 ⁰N. Hildebrand et al. (1990) introduced the Medial Zone terminology to account for the structure that was previously called Wopmay fault (Fig. 2; Easton 1981b; King et al. 1986). The Medial Zone interpretation (Fig. 2) suggests that rather than a fault, the zone is a series of folds and ductile fabrics that, to the west, become progressively transposed northward. Importantly, the Wopmay fault zone is a prominent topographic feature and structural break that is preserved throughout the length of the Wopmay orogen (Easton 1981b; Hoffman 1984; King et al. 1986; StOnge et al. 1991; Hoffman and Hall 1993; Jackson et al. 2006; Jackson 2008; Jackson and Ootes 2012). The Grant culmination occurs to the east of Wopmay fault zone (Figs. 1, 2, and 4) and is a teardrop shaped, anticlinal dome. Uraniumlead zircon ages from Grant culmination

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10 indicated it is older than >2.95 Ga (Hildebrand et al. 1990), and it was therefore considered to be part of the contiguous Slave craton (Figs. 1, 2, and 4; Hildebrand et al. 1991, 2010; map unit ‘my’ in StOnge et al. 1991; unit ‘A11’ in Hoffman and Hall 1993; unit ‘a’ in Hildebrand 2011). The Grant culmination is unconformably overlain by quartz arenite and pelite and because the basement was considered part of the Slave craton, these rocks were assigned to the Odjick Formation of the Epworth Group (Fig. 2; Hildebrand et al. 1990; unit P8 in Hoffman and Hall 1993; unit ‘weo’ in Hildebrand 2011). Critical to the Turmoil klippe model is a rock package east of Grant culmination that is referred to as Bent gneiss (Fig. 2). Bent gneiss is a mixed unit of graniteamphibolite and migmatitic gneiss that crystallized in the Archean and metamorphosed and deformed in the Proterozoic (unit ‘gn’ in StOnge et al. 1991; part of undivided unit ‘PA7’ in Hoffman and Hall 1993; part of undivided unit ‘wa’ in Hildebrand 2011). Bent gneiss is overlain by metasedimentary rocks and highgrade migmatites that have been assigned to the Akaitcho Group (Easton 1980, 1981a; King 1987; Hildebrand et al. 1991; StOnge et al. 1991; Hoffman and Hall 1993). Hildebrand andDraft Bowring (1988) mapped a mylonite zone east of Grant culmination, which was traced to the north and speculated to continue around the Grant culmination to the south and west (Fig. 2). This mylonite was considered to be a terrane bounding décollement, with the Grant culmination and Odjick Formation in the footwall, and the Bent gneiss in the hangingwall (Figs. 1C and 2; Hildebrand et al. 1990, 1991, 2010). The Bent gneiss was assigned to the Hottah terrane because of the discovery of four discordant zircons with 207 Pb/ 206 Pb ages between ca. 2.02 and 1.91 Ga, ages unknown in the Slave craton but considered typical of the Hottah terrane (Hildebrand et al. 1990). The interpretation of Slave craton and Coronation margin in the footwall and exotic Hottah terrane in the hangingwall led to the reinterpretation of the area that was previously considered as the metamorphic internal zone, as a klippe of Hottah terrane (Turmoil klippe; Fig. 2; Hildebrand et al. 1991, 2010). In contrast, bedrock mapping south of 65°N and UPb zircon dating of basement and sedimentary cover units (Bennett and Rivers 2006a; Jackson et al. 2006; Fyson and Jackson 2008; Jackson 2008; Bennett et al. 2012; Jackson and Ootes 2012; Jackson et al. 2013) highlighted that the crystalline Archean basement in the southern Wopmay orogen, and was deformed in the Paleoproterozoic, was most likely derived from the Slave craton. This result questioned the Turmoil klippe interpretation and further indicated that the Slave craton – Hottah

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terrane relationship required reevaluation (Jackson et al. 2013; Davis et al. 2015; Ootes et al. 2015).

METHODS Bedrock Mapping Bedrock mapping was undertaken between 64 ⁰N and 65 ⁰N and between Slave craton and the Phanerozoic platform (Fig. 1A; Jackson 2008; Jackson and Ootes 2012) in order to update the geological understanding of the area from earlier studies (e.g., Lord 1942; Frith 1973 and references therein; Easton 1981b; Frith 1986). Mapping at 1:100,000 scale, or better, began in 2004 and ended in 2012 (Jackson 2008; Jackson and Ootes 2012). This paper concentrates on the area between Slave craton and Wopmay fault zone (Fig. 4) and builds on the UPb zircon results in Bennett et al. (2012) and Jackson et al. (2013). The bedrock geology in two particular areas is relevant to this study. The first area is between Grant and Exmouth lakes (Figs. 45) and the second is in the vicinity of Rebesca LakeDraft (Figs. 4, 68). North of 65 ⁰N, reconnaissance traverses were conducted through Bent gneiss and near the Hepburn River in 2010 and 2011 by the first three authors.

Analytical Techniques Samples for UPb zircon geochronology (HIS1, Fig. 1; BG1, BG2, Figs. 4 and 5) were processed at the Geological Survey of Canada, Ottawa, ON, Canada. Zircon separates were analyzed by chemical abrasion isotope dilution mass spectrometry (CAIDTIMS; methods modified after Mattinson 2005) following the procedures described in Ootes et al. (2015). Monazite separates from one sample (BG2) were also analyzed by IDTIMS (not chemically or mechanically abraded). Sample dissolution and chemical methods are described in Parrish et al. (1987). Individual crystals were selected under a binocular microscope to avoid inclusions and other imperfections, spiked with a mixed 205 Pb233 U235 U tracer solution calibrated to ±0.1% against a gravimetric solution, and dissolved in highpressure bombs in HFHNO3. Data reduction and error propagation follow methods outlined in Roddick (1987). Accuracy and reproducibility of the ion counting measurements were monitored by analyses of the GSC standard 6266 with a 206 Pb/ 238 U ratio of 0.0963.

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Zircon separates from one sample (BG1; Figs. 4 and 5) and detrital zircons in sedimentary rocks (G, R, and W; Figs. 46) were analyzed by sensitive highresolution ion microprobe (SHRIMP II) at the Geological Survey of Canada, Ottawa, ON, following methods described in Stern (1997) and Davis et al. (2015) with standards and UPb calibration methods following Stern and Amelin (2003). All zircon grains were cast in 2.5 centimetre diameter epoxy mounts (GSC #318) along with fragments of the Geological Survey of Canada laboratory standard zircon (z6266, with 206Pb/ 238 U age = 559 Ma). For the detrital zircons, a random selection of 100 to 120 grains per sample, ranging from 50 to 100 m in size was selected. Detrital zircon grains were selected for analyses randomly, by following a grid pattern. All analyses were conducted using an 16 O primary beam and two different sized spots, one ca. 15 µm in diameter, and another ca. 9 µm in diameter, with a beam current of ca. 3.5 and 1nA, respectively. The 1 σ external errors of Pb/U ratios incorporate a ±1.0 % error in the standard calibration. Samariumneodymium isotope geochemistryDraft was completed at Carleton University following the procedures in Cousens (1996) and Hollings et al. (2012), and at the University of

British Columbia following the procedures in Weis et al. (2006a, b). Depleted mantle ages (T DM ) are calculated according to Goldstein et al. (1984).

RESULTS Basement Geochronology Bent Gneiss Foliated Tonalite (BG1) East of the Grant culmination is a mylonite zone (Figs. 2 and 4) first recognized by Hildebrand and Bowring (1988) and interpreted as a terrane bounding décollement, with the Hottah terrane in the hangingwall and Slave craton and Coronation basin strata in the footwall (Fig. 2; Hildebrand et al. 1990, 1991). The immediate footwall of the mylonite includes strongly deformed quartzite and siltstone, whereas the hangingwall is composed of gneissic granite, amphibolite, and metasedimentary rocks (Jackson and Ootes 2012). The mylonitic fabric is cut by granite dykes, but unfortunately samples of these dykes did not yield zircon. A sample of foliated tonalite, interpreted to have crystallized prior to deformation, was selected from the shear zone (BG1; Figs. 4 and 5).

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Zircons from the tonalite occur as euhedral to subhedral prismatic grains and backscatter electron imaging documents growth zoning typical of igneous zircon. Five analyses of chemicallyabraded single zircon grains yield <1% discordant data that define a discordia line (Fig. 9A; Table 1). As the spread in data is limited, a linear regression yields poorly defined upper and lower intercepts of 2602 ± 71 and 2114 ± 790 Ma, with considerable excess scatter. Anchoring the lower intercept at an age of 1870 ± 25 Ma, based on regional metamorphic data (see BG2 monazite data below), yields an upper intercept of 2589 ± 10 Ma. A minimum age is given by the weighted mean of the two oldest analyses at 2582 ± 1.1 Ma (Fig. 9A). To further assess the age of this sample, twentyseven zircons were analyzed by SHRIMP II. Twentytwo of 27 analyses yield a 207 Pb/206 Pb weighted mean age of 2584 ± 3 Ma (MSWD = 1.7), similar to the upper intercept age calculated by CATIMS (Fig. 9AB). Four of the excluded grains have slightly younger 207 Pb/206 Pb ages between 2540 and 2560 Ma (Table 2), presumably reflecting the Pbloss documented in the CAIDTIMS data set. Considering all the data, we interpret that this tonalite crystallized at 2584 ± 3 MaDraft (Figs. 5 and 9AB).

Bent Gneiss Foliated Granite (BG2) Complexly interlayered Archean granitic, amphibolitic, and migmatitic gneiss occur between Exmouth and Bent lakes (Figs. 46). These are unconformably overlain by migmatitic paragneiss, originally sedimentary rocks that were subsequently deformed and metamorphosed to upper amphibolite or possibly granulite facies (StOnge et al. 1991). A sample of strongly deformed basement granite was collected for UPb zircon dating (BG2; Figs. 4 and 5). Zircon occurs as euhedral to subhedral prisms. Five analyses of single zircon grains define a regression line with an upper intercept of 2581.8 ± 2.1 Ma and a lower intercept of 1168 ± 200 Ma (Fig. 9C). The three least discordant analyses, which overlap the Concordia curve (decay constant error included) yield a 207 Pb/206 Pb weighted mean age of 2578.1 ± 1.0 Ma. The upper intercept age is considered a maximum estimate for the age of igneous crystallization (Fig. 9C). Monazite from the sample was analyzed by TIMS, without undergoing chemical or mechanical abrasion. Three analyses of subhedral, pale yellow monazite crystals yield variable ages that define a regression line with an upper intercept age of 2582 ± 10 Ma and a lower intercept of ca. 1862 ± 5 Ma (Fig. 9D). The upper intercept age is consistent with the igneous crystallization age determined from the zircon analyses and the monazite data is interpreted to

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14 reflect complete to partial recrystallization of igneous monazite during a metamorphic event in the Paleoproterozoic. An accurate interpretation of the metamorphic age is limited by the small number of analyses. The youngest monazite analysis overlaps the concordia curve (0.2% discordant) at 1874.8 ± 1.5 Ma (Fig. 9D; Table 1). This age represents the maximum age of the metamorphic recrystallization, whereas the lower intercept age of 1862 ± 5 Ma is considered a minimum age for this event.

Hepburn Intrusive Suite (HIS1) A sample of strongly deformed to mylonitic biotite granite (HIS1; Fig. 1A) was collected from one of the most southerly exposed Hebpurn intrusive suite exposures documented in the Wopmay orogen, near the Hepburn River (Hoffman et al. 1980; StOnge et al. 1991; Fig. 1). Zircons from the granite occur as euhedral prismatic grains of varying quality. Six of seven single grain analyses define a regression line with an upper intercept age of 1892.4 ± 1.9 Ma (MSWD = 1.14) and a lower intercept ofDraft 301 ± 220 Ma (Fig. 9E). The excluded analysis has an older age of 1927 Ma that is interpreted to reflect an inherited grain (Fig. 9E). The zircon grains with highest optical quality are the least discordant (A101, 3; Table 1) and pin the upper intercept age (Fig. 9E; Table 1).

Sm-Nd Isotopes The Archean granitic basement rocks that occur south of 65 ⁰N have a tight range of 2580 εNd values between 0.5 to +1.0, with TDM ages between 2.75 and 2.92 Ga (Fig. 10; Table 3). 2580 The Bent gneiss sample (BG2) falls within this range, with εNd of 0.3. Deformed hornblendebiotite granodiorite plutons (ca. 1867 Ma) and Kfeldspar porphyritic granite (ca. 1863 Ma) that occur south of 65 ⁰N and intruded sedimentary rocks and Archean basement 1865 (Jackson et al. 2013), have εNd values between 3.4 to 4.7, and T DM ages of 2.49 to 2.59 Ga (Fig. 9; Table 3). Late orogenic, coarsely Kfeldspar porphyritic granitic plutons are not deformed (ca. 1858 to 1850 Ma; Jackson et al. 2013), and are isotopically more evolved than the 1855 older intrusive phases, with εNd between 5.4 and 7.2. They yield a range of TDM ages between 2.52 and 2.78 Ga (Fig. 10; Table 3), comparable to the Bishop suite plutons to the north (Fig. 10; Bowring and Podosek 1989).

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Detrital Zircon Geochronology Quartz Arenite Beds – Grant (G) and Rebesca (R) Lakes Quartz arenite beds occur within mixed marble, calcsilicate, pyritic psammite, and pelitic strata that unconformably overly deformed ca. 2580 Ma basement throughout the study area (Fig. 4; Jackson 2008; Jackson and Ootes 2012). On the southwest arm of Grant Lake (G) and at the south end of Rebesca Lake (R) quartz arenite was sampled (Figs. 48) for UPb detrital zircon analyses to constrain maximum deposition ages and assess zircon provenance (Fig. 11; Table 4). Quartz arenite samples from both locations yield predominantly Archean detrital zircon ages between 2.7 and 2.58 Ga with a younger cluster of Paleoproterozoic grains that indicate a maximum deposition age of 2030 ± 16 Ma (Fig. 11AB; Table 4).

Psammite Bed – Wopmay River (W) A cordieritebearing psammite (greywacke) bed was sampled from south of the Wopmay River and Little Crapeau Lake (W), whereDraft the metasedimentary rocks stratigraphically underlie a mafic sill that is thought to be related to the ca. 1893 Ma Grant Subgroup (Figs. 4 and 5; Jackson and Ootes 2012; Ootes et al. 2015). This sample yields detrital zircons with Archean ages similar to the previously discussed quartz arenite samples, in addition to a population of ca. 2.33 Ga, a most significant population at 1.97 Ga, and a smaller number of zircon grains at 1.93 Ga (Fig. 11C; Table 4). The maximum deposition age of this sample is 1920 ± 11 Ma (Fig. 11C), a 207 Pb/ 206 Pb weighted mean age derived from multiple analysis of the youngest identified zircon grain (n=8; analysis 10812038.x, Table 4).

DISCUSSION Parentage of Archean Basement in Wopmay Orogen The Turmoil klippe model advocates that Archean basement preserved west of the Slave craton (except the Grant culmination) belongs to the Hottah terrane (Figs. 1C3A; Hildebrand et al. 1991, 2010). That interpretation derived from studies north of 65°N, but it implies that all deformed Archean basement in the Wopmay orogen, including the extensive basement south of 65°N, is part of the Hottah terrane (Figs. 1C3Ae.g., Hoffman and Hall 1993). The model is based, in part, on the following: 1) there is a basal décollement around the western Slave craton (StOnge et al. 1991; Hildebrand et al. 1991, 2010); 2) there are Hottahlike zircon ages in the

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16 shear zone within the Bent gneiss (Hildebrand et al. 1990); 3) the Akaitcho Group unconformably sits on Bent gneiss, which is deformed and the state of deformation contrasts with that typical of the contiguous Slave craton (Hildebrand et al. 1991), and; 4) the Hepburn intrusive suite intrudes Akaitcho Group rocks and these plutons do not contain isotopic evidence of interaction with Archean lithosphere (Bowring and Podosek 1989; Housh et al. 1989; Hildebrand et al. 2010). Bleeker et al. (2000) has demonstrated that what was previously mapped as a Paleoproterozoic décollement around the Acasta area (Fig. 2) is actually an early Neoarchean shear zone, and the Paleoproterozoic sedimentary rocks sit unconformably on this Archean basement. Therefore an eastern décollement remains to be demonstrated (Bleeker et al. 2000) and it is removed on Figure 4. The Bent gneiss (Figs. 2 and 4) is a key feature to the klippe interpretation (Hildebrand et al. 1991, 2010). Hildebrand et al. (1990) reported four, non reproducible, discordant zircon analyses from a mixed gneissic unit and they interpreted a Paleoproterozoic age of 2.04 Ga for the monzodioritic component. Hildebrand et al. (1990) stated that “based on these ages gneissesDraft of unit a are considered to be part of Hottah terrane”. The foliated tonalite that occurs in the shear zone east of the Grant culmination (BG1) is dated here at 2584 ± 3 Ma and the deformed granite within the Bent gneiss (BG2) is dated at 2581.8 ± 2.1 Ma (Figs. 4,5, and 9AC). We found no evidence for Paleoproterozoic zircon in the two Bent gneiss samples, but there is evidence for Paleoproterozoic Pbloss, even in chemicallyabraded analyses (Fig. 9; Table 1). It is permissible that the discordant Paleoproterozoic ages in Hildebrand et al. (1990) may be due to the combined effects of metamorphism and Pbloss of older Archean material, potentially a result of isotopic resetting during metamorphism at 1.87 Ga, similar to the monazite ages preserved in the Bent gneiss (BG2; Fig. 9D). At the time of the earlier reports (late 1980’s), the technical ability to minimize, or isolate the effect of Pbloss or mixing in zircon, from strongly metamorphosed gneissic rocks was limited. During mapping, we were unable to find the Hildebrand et al. sample location, but we did determine that the area where the sample was collected is underlain by mylonite derived from a sedimentary protolith (Jackson and Ootes 2012). Also permissible, therefore, is that the reported Paleoproterozoic zircon ages may be detrital in origin, as they overlap the ages in the Wopmay River psammite (Fig. 11; Table 4). Either way, the previous geochronological data do not constitute conclusive evidence of what were considered to be diagnostic “Hottah” ages in the gneiss.

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The ca. 2682 Ma ages for the Bent gneiss are indistinguishable from the ages for the widespread Archean basement preserved to the south of 65 ⁰N in the Wopmay orogen (Figs. 46; Jackson et al. 2013). Jackson et al. (2013) advocated that this Archean basement was derived from the western Slave craton, not the Hottah terrane, because the UPb zircon crystallization ages match the ages of voluminous granitic plutonic rocks in the Slave craton (ca. 26002580 Ma; e.g., van Breemen et al. 1992; Davis and Bleeker 1999; Bennett et al. 2005; Ootes et al. 2005). A key Archean basement exposure in the Wopmay orogen is the composite gneiss at the south and east side of Rebesca Lake, which was deformed in the Paleoproterozoic (Figs. 68; also see figure 3C in Jackson et al. 2013). This gneiss has yielded a number of igneous zircon populations with ca. 2582, 2594, and 2620 Ma ages (Bennett et al. 2012; Jackson et al. 2013) and these match wellconstrained plutonic events in the adjacent Slave craton (e.g., van Breemen et al. 1992; Davis and Bleeker 1999; Bennett et al. 2005; Ootes et al. 2005). In further support of the Slavederived basement interpretation, Archean bedrock is not known in the Hottah terrane and there are only scant detrital zirconsDraft of Neoarchean age in Hottah terrane sedimentary rocks (Fig. 12; Bowring 1984; Davis et al. 2015; Ootes et al. 2015). The crystalline Archean basement rocks within the Wopmay orogen can further be linked to Slave craton on the basis of Nd isotopic data (Fig. 10; Table 3). They have relatively juvenile εNd 2580 values, indicating limited to no interaction with crust older than Mesoarchean. Although this contrasts with the signature of the Neoarchean plutonic rocks in the northwest and central part of Slave craton (e.g., Davis and Hegner 1992; Davis et al. 1996), the results are indistinguishable from post2.6 Ga plutonic rocks of the southwest Slave craton (Figs. 10 and 13). There, Neoarchean granites have relatively juvenile εNd 2590 of 0.5 to 2.0 (Yamashita et al. 1999; Bennett 2006; Buse 2006). It was previously advocated that the Mesoarchean Grant culmination (Figs. 1, 2, 4, and 5) was part of the Slave craton (Hildebrand et al. 1991, 2010). The UPb crystallization ages in Jackson et al. (2013) and this study (Fig. 8), as well as the Nd isotopic data (Fig. 9) support that the Neoarchean crystalline basement in the Wopmay orogen was also derived from the Slave craton. There are no geological reasons to make Archean exposures to the north any different (Fig. 13A; King et al. 1987), including the Badlands granite (67 ⁰11’N; cf. Hoffman et al. 2011).

Provenance of Paleoproterozoic Supracrustal Rocks

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An additional linkage between the basement domains within the Wopmay orogen and the Slave craton is the detrital zircon age populations in the unconformably overlying sedimentary rocks (Figs. 38, 11, and 12). Detrital zircon ages from two basal quartz arenites that were deposited on ca. 2580 Ma crystalline basement at Rebesca Lake and Grant Lake (R and G, respectively; Figs. 46), have maximum deposition ages of 2030 ± 16 Ma (Fig. 11), consistent with detrital input from the initial rift Melville Group (Fig. 12). The bulk of the detrital zircons in these two samples, however, yield Archean age populations (Fig. 11). These populations mirror results from correlatable quartz arenites, pelites, and volcaniclastic rocks from further south in the Wopmay orogen (Bennett et al. 2012; labelled Arm (A), Ingray (I), Mattberry (M), and Portage (P) on Figs. 4 and 12). Detrital zircon ages in these samples are typical of the Neoarchean igneous history of the Slave craton, including the prominent bimodal modes at ~2.6 2.58 and ~2.722.67 Ga (Fig. 12; e.g., van Breemen et al. 1992; Davis et al. 2015). The sampled units and intercalated stratigraphy (marble/calcsilicate, psammite, etc.) is similar to the descriptions of Akaitcho Group rocks thatDraft were deposited on deformed Archean basement north of 65 ⁰N (Easton 1980; 1981a, b; King 1987; King et al. 1987; StOnge et al. 1991; Hildebrand et al. 1991, 2010). The Wopmay River psammite (W) has yielded a distinct detrital zircon spectrum when compared to that of the quartz arenites sampled above the Archean crystalline basement (Figs. 11C and 12). While the psammite has a subdued Slavelike detrital zircon signature, it also contains younger Paleoproterozoic populations including a dominant agepopulation at ca. 1.97 Ga and a maximum deposition age of 1920 ± 11 Ma (Fig. 11C and 12). The Wopmay River psammite and associated pelites underlie the Grant Supgroup basalts and lesser rhyodacites, the date for which provides a minimum deposition age for the sedimentary rocks at ca. 1895 Ma (Figs. 3B5, 12; Ootes et al. 2015). The psammite differs from the Zephyr arkose of the Akaitcho Group, in that it does not contain the synvolcanic 1894.7 ± 0.9 Ma zircons (Hoffman et al. 2011). The relationship between the Wopmay River psammite (W) and the quartz arenites and associated sedimentary rocks (A, G, I, M, P, R; Figs. 36, 11, and 12) is either stratigraphic and the psammite represents a higher stratigraphic unit, or it is structural and the psammite and overlying basalts were thrust over the lower stratigraphy. The second possibility is considered less likely because we have found no evidence to suggest the presence of a fault (Figs. 3B5;

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Easton 1981b; Jackson and Ootes 2012). This leaves four possibilities regarding the age of the basal sedimentary rocks: 1) the basal quartz arenite sequence is correlative to the Melville Group riftsequence (ca. 2.01 Ga; Fig. 12); 2) they are correlative to the Epworth Group passive margin sequence (1.97 Ga); 3) they are part of the Epworth Group, but the Epworth Group is younger than previous correlations (Bowring and Grotzinger 1992), or; 4) the entire stratigraphic package was deposited around or after ca. 1.92 Ga and is correlatable to the Grant Subgroup/Akaitcho Group (Easton, 1981a,b). Scenarios 1 and 2 cannot be entirely ruled out because the detrital zircon results do not allow a unique solution. Scenario 3 is possible but testing these relationships is beyond the scope of this study. Scenario 4 seems the most likely. In support of scenario 4 is that there is no evidence of a structural (fault) or stratigraphic (unconformity) break between the basal stratigraphy and the Wopmay River psammite, and by description the entire sedimentary sequence is similar to previously described Akaitcho Group rocks to the north (ca. 1.9 Ga; Easton 1980; 1981a, b; Bowring 1984; King 1987; Hoffman 1984; King et al. 1987; St Onge et al. 1991). Further tangential supportDraft of the scenario 4 comes from insitu UPb chemical and isotopic dating. Pelitic rocks occur immediately above the basal quartz arenite and below the Wopmay River psammite in the vicinity of Grant and Little Crapeau lakes (Fig. 5). These pelites contain monazite grains that have ca. 1.88 Ga metamorphic ages, but they have internal zonations with older age domains between ca. 2.0 to 1.93 Ga (Smar 2015). Tectonic events related to these older ages are not recorded in the western Slave craton and metamorphic internal zone (Fig. 12) and these are best interpreted as detrital in origin, similar to the detrital zircon in the Wopmay River psammite. The results indicate the sequence was deposited after 1920 Ma and the basal stratigraphy received exclusively Slave and initial rift detritus, whereas higher stratigraphic levels (Wopmay River psammite) received detritus from more dynamic Archean Paleoproterozoic sources (Figs. 11 and 12). The timing of deposition of this strata, between 1920 and 1893 Ma, was concomitant with magmatism and extension in the Hottah terrane, including transition from the Hottah plutonic complex to Zebulon Formation volcanism in a rifting arc environment between ca. 1913 and 1900 Ma, and deposition of the overlying Conjuror Bay Formation quartzite at ca. 1900 Ma (Fig. 12; Ootes et al. 2015). The Grant Subgroup basalts that overlie the Wopmay River psammite are a temporal and geochemical match to the Bloom Basalts that directly overlie the Conjuror Bay Formation (Figs. 45, 11; Ootes et al. 2015). But, the detrital zircon record and underlying

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20 stratigraphy suggest differently (Figs. 3B and 12). First, the Wopmay River psammite is best interpreted as part of a relatively thin sedimentary cover sequence deposited on Archean crystalline basement, whereas the Conjuror Bay Formation overlies extensive ca. 1930 to 1900 Ma intrusive and volcanic rocks (Fig. 3B; Jackson 2008; Jackson and Ootes 2012; Jackson et al. 2013; Ootes et al. 2015). This is further mirrored in the detrital zircon record, where the Wopmay River psammite does not contain the prevalent ca. 1900 Ma detrital zircons that occur in the Conjuror Bay Formation (Fig. 12; Davis et al. 2015). While the Wopmay River psammite does have ca. 1.97 and 1.93 Ga detrital zircons, as do the sedimentary rocks in the Hottah terrane (Fig. 12; Davis et al. 2015), these ages are not unique to the Hottah terrane as they dominate the crust of the Thelon/Taltson magmatic zones that occur to the east and south of the Slave craton (Fig. 1; Davis et al. 2015). We therefore champion that the Wopmay River psammite has a Slave craton – Thelon orogen provenance. This is consistent with previous sedimentary models that predicted Thelonaged detritus within the Coronation margin (McCormick and Grotzinger 1993). The spatialrelationship with the similarDraft aged Hottah terrane is further discussed below.

Deformation of Basement in Wopmay Orogen The granitic rocks in the western Slave craton did not undergo ductile deformation after ca. 2.58 Ga (e.g., Pehrsson 2002; Bennett et al. 2005; Jackson et al. 2006). In contrast, the Archean basement rocks in the Wopmay orogen underwent extensive penetrative deformation after 2.58 Ga and generally contain complex deformation fabrics including folds, foliations, gneissosity, and lineations. This contrast in deformation state can be accounted for as follows. In the southern Wopmay orogen, the unconformity between the crystalline basement and overlying metasedimentary rocks is folded with the development of an associated axial planar foliation (Figs. 46; also see Fyson and Jackson (2008) and figure 3 in Jackson et al. 2013). Instructive examples of the basementcover thickskinned deformation were mapped at several localities, for example the southend of Ingray Lake where basement and cover form a largescale, north plunging synclinorium (Fig. 4), at Grant Lake, where the area is preserved as basementcored anticlinal domes and sedimentdefined synclines (Figs. 4 and 5), and at Rebesca Lake, where the map pattern indicates a refolded dome and basin structure (Figs. 4, 6, and 7). The penetrative deformation was polyphase and was associated with metamorphism between greenschist and granulite grade, and bracketed between ca. 1877 and 1850 Ma (Jackson et al. 2013; Smar 2015).

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There is evidence that some of the crystalline basement may have been deformed prior to deposition of overlying sedimentary rocks. At the south end of Rebesca Lake (Fig. 6) the

Archean crystalline basement contains a strong gneissic to mylonitic fabric (S gn ) that is parallel

to S0 in the overlying metasedimentary strata (Figs. 67A). The strain state in these sedimentary

rocks is nowhere as strong as in the crystalline basement (Figs. 68). As well, if Sgn had

developed after the deposition of the overlying strata, then the fabric should cut S0 in fold hinges

(F 1 or F 2; Fig. 7B), which it does not (Fig. 7C). This is collectively taken as evidence that the S gn

fabric likely formed prior to the deposition of the overlying strata (S0). Not all basement exposures are as strongly deformed as the Rebesca gneiss, indicating the Archean basement underwent heterogeneous strain prior to deposition fo the overlying stratigraphy. The timing of

Sgn deformation is difficult to constrain because of metamorphic and structural overprinting, when datable minerals such as monazite were reset (Fig. 9D; Jackson et al. 2013; Smar 2015). It is possible that the deformation occurred during the late Archean, after ca. 2.58 Ma. In the Rebesca gneiss, Bennett et al. (2012) documentDraft a population of ca. 2.57 Ga zircon grains and rims, and interpret these as metamorphic in origin and so it is possible the S gn fabric is related to ca. 2.57 Ga deformation processes – there is evidence in the Slave craton that plutonic and thermal events continued to ca. 2.55 Ga (Davis et al. 2003a; Bleeker et al. 2007). If this is the case, the basement exposures in the Wopmay orogen could represent a deeper crustal section than is preserved in the adjacent craton, which was exhumed prior to deposition of the overlying

sedimentary rocks. An alternative interpretation is that the S gn could have developed from extensional shear during exhumation immediately prior to or synchronously with the opening of a basin capable of accommodating the overlying supracrustal rocks (Fig. 6C). The absolute timing of this presedimentation deformation remains to be thoroughly tested and should be the focus of future research.

A Rifted Cratonic Margin The Coronation margin was established by rifting of the western Slave craton at ca. 2.02 Ga (Fig. 14), inferred in part from the age of the Lac de Gras dyke swarm and associated Booth River intrusive suite (Roscoe et al. 1987; Hulbert 2005; Hoffman et al. 2011). Deposition of the Melville Group at ca. 2.014 Ga represents the rift to drift transition, but is only preserved in a narrow northstriking anticline in the northern Wopmay orogen (Bowring and Grotzinger 1992;

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Hoffman 1996; Hoffman et al. 2011). The deposition of the passive margin sedimentary rocks of the Epworth Group is considered to be ongoing at ca. 1.97 (Figs. 12 and 14), as constrained by correlation to the Kilohigok basin to the east (Bowring and Grotzinger 1992). The transition within the Grant Subgroup/Akaitcho Group at ca. 1.9 Ga, from basal quartz arenite, marble/calc silicate to more extensive rusty psammite and pelite, and finally to pillow basalt (Fig. 3B), is best interpreted as a deepening basin. This is consistent with a renewed or second rift event between 1.92 and 1.89 Ga (Fig. 14). Easton (1980, 1981a, b) interpreted the Grant/Akaitcho as a riftrelated sequence, but considered it to be the basal rift of the Coronation margin (Hoffman and Bowring 1984). Subsequently the Melville Group was shown to document initial rifting of the western Slave craton (Fig. 14; Bowring and Grotzinger 1992; Hoffman et al. 2011). The Grant/Akaitcho sequence necessarily defines a second rift phase (Fig. 14). Multiple extensional phases are documented in many passive margins (e.g., Masini et al. 2013; Bell et al. 2014) and numerical modeling demonstrates that riftaxis migrationDraft can occur after cooling of an initial rift during continental breakup (Naliboff and Buiter 2015). This may be the situation in the Wopmay orogen. After initial rifting at 2.03 to 2.01 Ga, the lithosphere underwent slow cooling during the passive margin phase and rheological hardening resulted in riftaxismigration, or reactivation at ca. 1.92 Ga. The new 1892.4 ± 1.9 Hepburn intrusive suite age (Fig. 9E) overlaps with basaltic volcanism in the Grant Subgroup at 1892.9 ± 1.4 Ma (Ootes et al. 2015) and the 1894.7 ± 0.9 Ma maximum deposition age of the Zephyr arkose of the Akaitcho Group (Hoffman et al. 2011). The results support the onset of a second phase of rifting at or after ca. 1.92 Ma and maximum extension of the rift at 1.89 Ga (Fig. 14). The crystalline Archean basement was exposed at the onset of riftrelated sedimentation (Figs. 48 and 14) and both were structurally overprinted by compressional deformation between ca. 1877 and 1860 Ma (Jackson et al. 2013; Smar 2015). During the rifting and later deformation, the adjacent Slave craton was not susceptible to penetrative deformation and remained structurally rigid. As such, the Archean basement in the Wopmay orogen had to have been weakened to the point where it was vulnerable to multiple stages of penetrative deformation. But how can previously cratonized crust be weakened? Extensional environments, whatever their cause, may provide the answer (e.g., Kusky et al. 2014), as these environments thermally weaken the lithosphere, thus permitting subsequent contractional deformation during collision (e.g.,

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Vacherat et al. 2014, 2016). We interpret that the rifting phases stretched, exposed, and thermally weakened the Archean basements lithosphere (Fig. 14). Once stretched and thermally perturbed, previously cratonized Archean lithosphere and overlying Paleoproterozoic stratigraphy was then susceptible to compressionrelated ductile deformation during the Calderian orogeny. This orogeny is related to subduction processes that formed the Great Bear magmatic zone, providing another thermal and metasomatic overprint. The relatively sharp boundary between deformed Archean crust in the Wopmay orogen and undeformed Archean crust in the Slave craton (Figs. 1, 4, and 13; Pehrsson 2002; Jackson et al. 2006) is interpreted as the eastern rift boundary (Fig. 14) and this boundary acted as a rigid backstop during the forthcoming contractional deformation (Fig. 14). The timeframe from the second rift phase, and associated thermal weakening, to imbrication is ca. 30 million years (Figs. 13 and 14). This is comparable in time to Phanerozoic analogues, for example in the Pyrenees (Vacherat et al. 2014). As the thermal structure of a rift is generally wedgeshaped (Fig. 13B; Naliboff and Buiter 2015) the crust of the western Slave craton was spared from this riftrelated Draftthermal weakening, but the mantle may not have been. The ca. 1.92 to1.89 Ga extensional phase described above temporally overlaps a rift sequence documented in the Hottah terrane (Ootes et al. 2015). The Grant Subgroup and Bloom Basalts are correlatable and cap the older stratigraphy (Figs. 3B and 12), representing a period when extensiondriven magmatism overtook sedimentation. The units under those basalts are a temporal match, but they do not share stratigraphic, petrologic, or provenance similarities (Figs. 3B and 12). While the temporal coincidence hints that these were part of the same largescale rifting event the difference in the nature of the underlying crust indicates that they were geographically separated, perhaps by hundreds to thousands of kilometers (Davis et al. 2015; Ootes et al. 2015). These authors used the detrital zircon record and petrological evolution of the Hottah terrane to suggest that it began as the rifted margin of the Taltson or Ksituan magmatic zones, significantly to the south of the Coronation margin and Slave craton. They imply that basin opening and transtensional shear drove the birth of the new Hottah terrane. The temporal match between 1.92 and 1.89 Ga, but differing provenance (Fig. 11) implies that the Hottah terrane and the westernmost Slave craton, now preserved within the metamorphic internal zone of the Wopmay orogen, both experienced some largescale extension of a compound continental margin. The driving mechanism of the extension remains unresolved, but new 4D modelling reveals that a plateau or microcontinent may have collided to the south around ca. 1.92 Ga,

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24 along the Taltson or Ksituan margin (Ootes et al. in press). Such a collision would temporarily shutdown the subduction system and put the crust into extension, a model that accommodates the birth of the Hottah terrane at that time (Davis et al. 2015; Ootes et al. 2015). Propagation of this activemargin rift to the north could account for the second rift along the western Slave margin (see figure 11 in Ootes et al. 2015). Arrival of the Hottah terrane and inversion of the rift began at ca. 1.88 Ga, coeval with Recluse Group foredeep sedimentation, deposition of the Treasure Lake Group, and onset of the Calderian orogeny (Fig. 12; Gandhi and van Breemen 2005; Bennett et al. 2006b; Hildebrand et al. 2010; Hoffman et al. 2011; Jackson et al. 2013). This orogeny included polyphase magmatism plutonism, deformation, and metamorphism between ca. 1877 and 1850 (Bowring 1984; Jackson et al. 2013; Smar 2015) and was synchronous with the development of the Great Bear arc, constructed by subductioncollision processes to the west (Fig. 12; Hildebrand et al. 1987, 2010; Gandhi et al. 2001; Ootes et al. 2015; Ootes et al. in press). The Nd isotopic signatures of the Paleoproterozoic plutons appear to ‘track’Draft the evolution of the latest stages of the rifting and the subsequent convergent history (Fig. 10). The relatively juvenile Nd isotopic record of the Hepburn intrusive suite indicates emplacement into a cratondistal, fully attenuated basin (Lalonde 1989). In the southern Wopmay orogen, the Zinto suite plutons were emplaced at ca. 1867 Ma (Jackson et al. 2013) and coincide with subductionrelated plutonism in the Great Bear magmatic zone to the west (Bowring 1984; Hildebrand et al. 1987, 2010; Gandhi et al. 2001; Ootes et al. 2015). The Zinto plutons have a more evolved isotopic signature than the Hepburn intrusive suite (Fig. 10), but do not have a strong Archean signature, with T DM ages around 2.5 Ga (Table 3). The Zinto suite Nd isotopic values could be derived from this subductionmodified mantle (Archean?), possibly mixed with minor amounts of either Paleoproterozoic or Archean crust (Fig. 10). Collectively, these plutons and the older supracrustal rocks and Archean basement were deformed (Jackson et al. 2013) as a consequence of oblique collisional processes to the west (Hildebrand et al. 1987; Ootes et al. 2015). The Bishop intrusive suite granitic plutons represent the final magmatic pulse between ca. 1858 and 1850 Ma (Bowring 1984; Jackson et al. 2013), and are more evolved than the older plutons (Fig. 10). This supports that Archean crust may have played a more significant role in their source or contamination (Fig. 10; Bowring and Podosek 1989; Housh et al. 1989). In summary, the plutonic phases trace an

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evolution from maximum rifting at ca. 1892 Ma, to inversion between ca. 1880 and 1860 Ma, and magmatic shutdown by ca. 1850 Ma.

Implications for On-Craton Diamonds The Slave craton contains worldclass kimberlitehosted diamond deposits. To date, no oncraton kimberlite (diamondbearing or not) has been discovered west of about 114 ⁰W longitude (Figs. 1A and 13). The Slave craton was extensively explored for kimberlite in the 1990’s, and as diamonds are rare and kimberlite is friable, a key tool for hunting diamond bearing kimberlite is the use of kimberlite indicator minerals in glacial till (LeCheminant et al. 1996). Identification of prospective indicator minerals, such as peridotitic and eclogitic garnet, within glacially dispersed mineral trains, help track diamondbearing kimberlite (Shulze 2003). During exploration, sampling grids that lack prospective indicator minerals are typically abandoned. By deduction, if there were motivating indicator mineral trains in the western Slave craton or eastern Wopmay orogen (Fig.Draft 13), then exploration for diamondiferous kimberlite would remain active, but such exploration has all but ceased in this area. Consequently, while undiscovered oncraton kimberlite may exist, a lack of amenable diamondindicator minerals likely indicates a lack of diamond potential. Given the current state of knowledge, it is incumbent that we provide a geological reason why the western Slave craton appears to be diamondsterile. An essential condition for diamond preservation in the mantle is a thick and relatively cold subcontinental lithospheric root, and it is generally accepted that this root formed during the Archean or Proterozoic (Pearson and Wittig 2008; Heaman and Pearson 2010). This is well preserved beneath the diamondrich central part of the Slave craton (Stachel et al. 2003; Heaman and Pearson 2010; Snyder et al. 2014). Rifted environments have wedgeshaped thermal structures (Fig. 13B; Naliboff and Buiter 2005) such that the subcontinental lithospheric mantle under the western Slave craton would have been thermally perturbed at ca. 1.9 Ga while the crust above it could have remained rigid, at least to the point where the crust transitioned to the rift edge, ie., the boundary with the deformed Archean basement in the Wopmay orogen (Figs. 4, 13, and 14). Riftrelated thermal overprinting would accentuate geothermal gradients, potentially moving the mantle out of the diamond to the graphite stability field (e.g., Kennedy and Kennedy 1976). The subsequent imbrication and metamorphism of the crust in the Wopmay orogen

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26 implies that what remained of the heated mantle was structurally and metasomatically overprinted again during the Calderian orogeny. Therefore, while Archean lithosphere is well preserved in the western Slave craton (e.g., Jackson et al. 2006; Spratt et al. 2009) perhaps the subcontinental lithospheric root most proximal to the rift edge (Fig. 13) suffered irrevocable overprinting affects during these Paleoproterozoic processes, rendering it diamond sterile. If this hypothesis is correct it would further support that postcratonization effects are important considerations for oncraton diamond preservation. The attenuated and imbricated Archean crust preserved in Wopmay orogen helps explain why the western part of the Slave craton, at least as far as it is currently known, lacks the diamondfertility of the central and eastern part of the carton. While it is promoted that the western Slave craton is diamondsterile, two cautionary notes are worth considering. Firstly, early maps of the Wopmay orogen showed only minor amounts of Archean basement (e.g., Hoffman 1984); only more recently has it been demonstrated that Archean basement isDraft relatively extensive, particularly evident in the southern part of the Wopmay orogen (StOnge et al. 1991; Bennett and Rivers 2006a; Jackson 2008; Hoffman et al. 2011; Bennett et al. 2012; Jackson and Ootes 2012; Jackson et al. 2013). This lack of knowledge could have played a major factor in directing exploration in the 1990’s and it remains possible that the western Slave region and Wopmay orogen is dramatically underexplored. Secondly, exploration may have overlooked the possibility of offcraton diamondiferous lamproite, like those that host the Argyle diamond mine in the Halls Creek orogen, Australia.

CONCLUSIONS The original designation of the rocks between Wopmay fault zone and Slave craton to a metamorphic internal zone (e.g., Hoffman 1984; King 1987; King et al. 1987; StOnge and King 1986, 1987) is consistent with the preserved geology. The field, UPb, and Nd isotopic evidence presented in this study and in Jackson et al. (2013) supports that the Archean crystalline basement in the Wopmay orogen has a western Slave craton parentage. This is further supported by the detrital zircon provenance record in the unconformably overlying sedimentary cover sequence. Henceforth, the Turmoil klippe, and associated terminology is no longer applicable. The initial rifting of the Wopmay orogen began at ca. 2.02 Ga and transitioned to a passive

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margin at ca. 1.97 Ga (Bowring and Grotzinger 1992; Hoffman et al. 2011). The second rift phase was filled with supracrustal rocks of the Grant Subgroup/Akaitcho Group, and detrital zircon results indicate a Slave craton provenance for the basal quartz arenites, with additional Thelon/Taltson aged zircons in stratigraphically higher rocks (Fig. 12). A maximum deposition age of ca. 1920 Ma constrains the onset of rifting and the maximum extent is taken to coincide with the extrusion of pillow basalts at ca. 1893 Ma (Ootes et al. 2015) and intrusion of the Hepburn intrusive suite, dated herein at 1892.4 ± 1.9 Ma and potentially continuing to ca. 1880 Ma. This second rift sequence is a temporal match to a rift sequence documented in the adjacent Hottah terrane (Ootes et al. 2015). However, the stratigraphy below the upper basaltic rocks and the disparate detrital zircon records indicate that these sequences evolved on different stratigraphic basement and therefore preserve the distal components of a rifted margin (Fig. 3B). The underlying driver of rifting was probably largescale platereorganization that affected the composite western Slave and Taltson margin between ca. 1.92 to 1.89 Ga (Davis et al. 2015; Ootes et al. 2015; in press). Draft Lithospheric thermal weakening during rifting allowed the Archean basement, along with the overlying supracrustal rocks and early intrusions, to later be deformed during compression related to the Calderian orogeny, between ca. 1.88 and 1.85 Ga. The boundary between Slave craton and deformed Archean crystalline basement within the southern Wopmay orogen is relatively sharp (Figs. 4 and 13) and we interpret that it demarcates the eastern border of the second rift. This rift edge, the western Slave craton, acted as a rigid backstop during the compressional stages. The Nd isotope signature in the plutonic phases track the extent and evolution of the rifted margin, from isotopically juvenile at ca. 1892 Ma to isotopically evolved at ca. 1855 Ma. The older plutons record the riftmaximum and the younger plutons are related to the Calderian orogeny, formed by eastdirected subduction processes that also led to plutonism in the Great Bear magmatic zone, preserved to the west. The ca. 30 million year timeframe from rifting to the onset of compression at ca. 1.88 Ga is similar to that postulated for thermal weakening in an extended margin (Vacherat et al. 2014), as originally proposed for this region (StOnge and King 1986, 1987; Lalonde 1989). This study provides a reasonable explanation as to why the western Slave craton (west of 114°W) appears to be diamondfree. The crust of the western Slave craton was not penetratively deformed after the Archean, but the correlative Archean crystalline basement in the Wopmay

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28 orogen was, a result of rifting and thermal weakening. Rifted margins have wedgeshaped thermal profiles and it was likely that the western Slave craton’s lithospheric mantle was thermally weakened by elevated geothermal gradients between ca. 2.02 and 1.89 Ga (Figs. 13 and 14). This was overprinted again by subductionrelated processes between 1.88 and 1.85 Ga. We postulate that while the western Slave craton may contain undiscovered kimberlite, the processes depicted shifted the lithospheric mantle from the diamond to the graphite stability field, rendering the western margin of the Slave craton diamond sterile (Fig. 13).

ACKNOWLEDGEMENTS This study forms part of the South Wopmay bedrock mapping project by the Northwest Territories Geological Survey (contribution #0097) and was supported in part by the Geological Survey of Canada GEM project (ESS cont. #) and Polar Continental Shelf Projects (500 07, 50709, 00410, and 31311). Expert field assistance pertinent to this study was provided by D. Mackay, M. Hewton, B. Williams, andDraft D. Knowlton. We thank E.A. Spencer for acquisition of the Nd isotope data at the Carlton University laboratory and D. Weiss and R. Tosdal from the UBC laboratory. M. StOnge provided a thorough and constructive review on an early version of this manuscript and T. Kusky and Associate Editor F. Corfu on behalf of the journal. We thank A. Polat and the editorial staff for timely and expert handling of the paper.

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TABLES Table 1. UPb zircon CAIDTIMS results Table 2. UPb zircon SHRIMP II results (Sample GB1) Table 3. SmNd isotopic results Table 3. UPb detrital zircon SHRIMP results

FIGURE CAPTIONS Figure 1. A) Location map of Slave craton and Wopmay orogen. Sample locations in this study are denoted. WFZ – Wopmay fault zone; GBL – Great Bear Lake; GSL – Great Slave Lake Two interpretations for the area east of Wopmay fault zone and west of Slave craton are B) a klippe of Hottah terrane and C) a metamorphic internal zone. gc – Grant culmination. Modified after Hoffman and Hall (1993).

Figure 2. Map depicting the Turmoil klippe interpretation, where Grant culmination is assigned to the Slave craton and all other units, except the ca. 1850 Ma Bishop intrusive suite, were

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38 assigned to the Hottah terrane. Hildebrand and Bowring (1988) identified the mylonite zone (marked) and traced an enveloping décollement around the Grant culmination. UPb zircon sample locations from Hildebrand et al. (1990) are located by black dots. The geology is modified after Easton (1981b), StOnge et al. (1991), and Jackson and Ootes (2012). The tectonic and stratigraphic assignments are from Hildebrand et al. (1990, 1991, 2010), Hoffman and Hall (1993), and Hildebrand (2011). Note that the geology south of 65 ⁰N is modified for the purpose of this figure and shaded lighter (after interpretations in Easton 1981b). See Figures 4 and 5 for an alternative geological interpretation of this area. AR – Acasta River; BL – Bent Lake; EL – Exmouth Lake; GL – Grant Lake; TL – Trumoil Lake; WL – Wopmay Lake.

Figure 3. A) General stratigraphy of the Coronation margin and the Turmoil klippe stratigraphy. Constructed using details from Bowring (1984), Bowring and Grotzinger (1992), Hildebrand et al. (2010), and Hoffman et al. (2011). The stratigraphic relationships between the left and right side of the panel are ruled out in this study.Draft B) Generalized stratigraphy of the Hottah terrane (modified after Reichenbach 1991; Davis et al. 2015; Ootes et al. 2015) compared with the metamorphic internal zone in the southern Wopmay orogen, the area between the Slave craton and the Wopmay fault zone (simplified from results in Jackson 2008; Jackson and Ootes 2012). G (Grant quartz arenite), R (Rebesca quartz arenite), and W (Wopmay River psammite) correspond to detrital zircon samples in this paper.

Figure 4. A) Geology between Wopmay fault zone and Slave craton in the southcentral Wopmay orogen. Geology south of 65°N is simplified after Jackson (2008) and Jackson and Ootes (2012). Geology north of 65°N is simplified after StOnge et al. (1991). Map boundary faults are not adjusted. Age controls are from Jackson et al. (2013) and detrital zircon sample locations are from Bennett et al. (2012). Other age constraints are from Bowring (1984), Harlan et al. (2003), Hildebrand et al. (1990), and Ootes et al. (2015). Blue lines 1ABC, 2ABC, 3A BC, 4AB are cross section traces. B) Cross sections through the study area corresponding to blue section lines in (A). Topography is vertically exaggerated 10x. The figures are schematic below approximately 100 m depth from surface exposure (MASL = meters above sea level). Sample location abbreviations: BG1, 2 – Bent gneiss; G – Grant Lake quartz arenite; R – Rebesca Lake quartz arenite; W – Wopmay River psammite; P – ‘Portage’ Lake volcaniclastic

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and quartzite; A – ‘Arm’ Lake pelite; I – Ingray Lake quartzite; M – Mattberry Lake quartzite. Lake name abbreviations: BLL – Black Lichen; EL – Exmouth; GL – Grant; IL – Ingray; ML – Mattberry; LCL – Little Crapeau; ReL – Rebesca; RL – Rodrigues; TL – Turmoil; WL – Wopmay; ZL Zinto .

Figure 5. Bedrock mapping results in the Grant and Exmouth lake areas. Geology north of 65 ⁰N is modified after StOnge et al. (1991) and south of 65 ⁰N is simplified after Jackson and Ootes (2012) with modifications after Easton (1981b). Age controls include one Mesoarchean age from Hildebrand et al. (1990). Other Archean basement and Paleoproterozoic intrusive ages are from Jackson et al. (2013) and the Grant Subgroup age is after Ootes et al. (2015). Compare unit assignments south of 65 ⁰N with Figure 2.

Figure 6. A) Bedrock mapping results in the Rebesca Lake area (simplified after Jackson and Ootes 2012). UPb zircon ages are fromDraft Bennett et al. (2012) and Jackson et al. (2013). The supracrustal rocks were metamorphosed between amphibolite (andalusitein to sillimanite + meltin) to possibly granulite grade (olivineinmarble); however, preservation is generally at amphibolite grade. Units are separated based on compositional variations within the sedimentary package. The timing of the Hottah sheet is from Harlan et al. (2003).

Figure 7 A) Structural interpretation of the southern Rebesca Lake area. Only deformed Archean

basement is filled (grey). S gn = gneissic layering/foliation in Archean basement, S 0 =

unconformity surface and bedding in immediately overlying sedimentary rocks, F 1 and F 2 = first and second generation fold axis, respectively, and ? = unknown relationships due to poor

preservation and exposure. B) Upright F 1 fold schematically demonstrating that if S gn formed

during first stage of folding it would be parallel to the F 1 fold axis (S 1) and crosscut the

unconformity in F1 folds. C) Scheme of S gn related to extension and exhumation of the basement,

forming prior to sedimentation, accounting for the general parallel nature of S gn and S 0 in the Rebesca Lake area.

Figure 8. Outcrop photographs of stratigraphy at the south end of Rebesca Lake (see Figure 6 for

geology map). A) Neoarchean (ca. 2582 Ma) granitic gneiss to mylonitic (S gn ). View is east.

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Also see figure 3C in Jackson et al. (2013). B) Marble with shallowdipping beds (S 0) about 50 metres above unconformity with underlying Archean gneiss. View is east. Photograph of the unconformity is in Jackson et al. (2013, figure 3I). C) Quartz arenite, in this case stratigraphically above the marble, with wellpreserved bedding (S 0). This is detrital zircon sample location R. View is north. D) Rusty psammite, mixed with pelite on a small island stratigraphically above the marble and quartz arenite. Thin Hottah sill (780 Ma) with columnar joints postdates all deformation and is bedding (S0) parallel. View is north. Of note is the relatively high strain preserved in the basement gneiss versus the relatively lower strain preserved in the unconformably overlying sedimentary rocks.

Figure 9. Concordia plots of UPb zircon and monazite. A) CAIDTIMS results of zircon in Bent gneiss tonalite (BG1), from the shear zone east of the Grant culmination. B) SHRIMP II zircon results from sample BG1. C) CAIDTIMS results from granite in Bent gneiss (BG2) from northwest of Exmouth Lake. D) TIMSDraft monazite results from sample BG2. E) CAID TIMS results from Hepburn intrusive suite (HIS) sample from the Hepburn River area. CAID TIMS results are in Table 1 and SHRIMP II results in Table 2.

Figure 10. A) Age vs. εNd T for reworked Archean granite and younger intrusive phases in the Wopmay orogen. B) Closeup showing that as age of plutons decrease the εNd T becomes progressively more evolved. Age controls from this study and Jackson et al. (2013). Hepburn Intrusive suite and Bishop Intrusive suite data are from Bowring and Podosek (1989). The southwest Slave craton data are from Yamashita et al. (1999), Bennett (2006), and Buse (2006). Depleted mantle bracketed from DePaolo (1981) and Goldstein et al. (1984).

Figure 11. 207 Pb/ 206 Pb age versus probabilitydensity plots for SHRIMP detrital zircon results that are 95% to 105% concordant. Grey filled probability curves includes data that is 90% to 110% concordant. A) Detrital zircon UPb results from the Grant Lake quartz arenite (G). B) Detrital zircon UPb results from the Rebesca Lake quartz arenite (R). C) Detrital zircon UPb results from the Wopmay River psammite (W). Age probability peaks are identified in Ga. Arrows and numerals at bottom right of panels indicate older detrital zircon grains that were dated but not plotted. See Figures 46 for sample locations.

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Figure 12. Comparison of the Slave craton, metamorphic internal zone, and Hottah terrane provenance. Slave craton crystallization ages and detrital zircon record of the Hottah terrane are modified after Davis et al. (2015). The Slave craton igneous crystallization age errors have been adjusted to ±10 Ma (1 σ) in order to be comparable to detrital zircon results (Davis et al. 2015). The Archean basement ages for the metamorphic internal zone are from Hoffman et al. (2011), Jackson et al. (2013), and this study (see Fig. 8). Plutonic and volcanic age constraints are from Bowring (1984), Gandhi and van Breemen (2001), Bennett et al. (2006a), Hoffman et al. (2011), and Ootes et al. (2015). Tectonic assignments for the provenance of the Hottah terrane are modified after Hildebrand et al. (2010), Davis et al. (2015), and Ootes et al. (2015) and for the metamorphic internal zone and Slave craton are modified from Easton (1981a), Bowring and Grotzinger (1992), van Breemen et al. (1992), Davis and Bleeker (1999), Hildebrand et al. (2010), Hoffman et al. (2011). Other sources are identified on the figure. Metamorphic internal zone detrital zircon sample locations areDraft on Figure 4.

Figure 13. A) Slave craton boundary map showing Archean exposures in the Wopmay orogeny, Slave Nd isotopic lines, documented oncraton kimberlite occurrences (black triangles), and kimberlitehosted diamond mines (white diamonds). Oncraton kimberlites have not been discovered to the west of the thick dashed line. Neodymium isotope lines (Nd) delimit the central extent of the Meoarchean and older Central Slave Basement Complex to the central part of the craton; there is no evidence of older crust in the southwest or east of the craton (after Davis and Hegner 1992; Yamashita et al. 1999; Buse 2006). Geology is modified after Hoffman (1984), St Onge et al. (1991), Stubley (2005), Jackson (2007), and Jackson and Ootes (2012). B) Thermal and structural profile of a rift after ca. 24 Ma of extension (modified after Naliboff and Buiter 2015). The figure is placed off the left side and scaled with (B) to demonstrate how the lateral and vertical distances a riftrelated thermal wedge may have affected Slave craton lithosphere during Paleoproterozoic rifting.

Figure 14. Proposed evolutionary model for the metamorphic internal zone of Wopmay orogen. A) Initial rift of Slave craton at ca. 2020 Ma (Hoffman et al. 2011). B) Passive margin sedimentation at ca. 1970 Ma, correlated from the tuff ages and stratigraphy in the Kilohigok

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42 basin (Bowring and Grotzinger 1992). C) A second rifting phase between ca. 1920 and 1890 Ma led to exposure of the Archean basement and deposition of the Grant Subgroup/Akaitcho Group sedimentary and volcanic rocks, , and emplacement of the Hepburn intrusive suite (HIS). D) Circa 18801850 Ma imbrication and emplacement of plutons, including the Zinto intrusive suite and Bishop intrusive suite. Age constraints from Jackson et al. (2013) and Smar (2015). Figures are schematic.

Draft

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o o 120 68 104o A 68o Coppermine HIS-1 sample Homocline location

Zone BG-1 & 2 Kilohigok GBL WOPMAY sample location OROGEN basin

Magmatic G, R, W

sample location Thelon SLAVE WFZ CRATON

Western limit of

B & C on-craton kimberlite

East Arm Yellowknife basin 1000 km Phanerozoic Platform GSL Rae Province

0 50 100 Kilometers 60o o Taltson o 120 Magmatic Zone 60 104o B C Asiak Asiak

fold-thrust belt Draft fold-thrust belt Hottah Hottah terrane terrane klippe

internal zone

Turmoil metamorphic Slave gc Slave gc craton craton

Great Bear magmatic zone Great Bear magmatic zone

Wopmay fault zone Wopmay fault zone Wopmay

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Slave Craton Turmoil Klippe

Medial Zone mylonite zone

Draft Gneissic

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A Turmoil klippe Coronation margin

Recluse Gruop (ca. 1882 Ma) Akaitcho Group/ Epworth Group (ca. 1970 Ma) Grant Subgroup (ca. 1900 Ma) Hottah terrane (including Melville Group (ca. 2014 Ma) Archean basement) Slave craton (>2580 Ma)

Hottah terrane East of Wopmay B west of Wopmay fault zone fault zone

Bloom Basalt 1895 ± 2.3 Grant Subgroup 1892.9 ± 1.5 Fishtrap Gabbro gabbro sills (dykes and sills) Conjuror Bay W <1920 ± 11 (DZ) Formation <1900 ± 11 (DZ) Zebulon Formation 1905.6 ± 1.4

sequence Bell Island Bay Group Beaverlodge G & R <2030 ± 16 (DZ) Lake sandstone

Coronation margin Hottah plutonic Draft 1912.9 ± 0.7 Archean complex 1930 ± 1 basement Holly Lake >2575 metamorphic <1951±15 (DZ) complex Supracrustal rock types Plutonic rock types unconformity 2030 ± 16 - Age (Ma) ± 2s Pillow basalt Pelite/psammite Gabbro/amphibolite this study Subaerial basalt Arenite & conglomerate Hottah plutonic rocks 1930 ± 1 - Age (Ma) ± 2s Subaerial rhyolite Marble & calc-silicate Archean basement previously reported DZ - detrital zircon Pelite and metabasalt Quartz arenite maximum deposition age

Figure 3. Ootes et al.

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116°W 115°W

C Acasta gneiss Slave >4.0 Ga WL craton

^_BG-2 TL

Bent EL gneiss 65°N 65°N ^_BG-1 c G ulm ran inat %, t %, GL ion 2590 2576 B 1A %, XY G 2583 LCL RL 2A XY W Draft RXY U-Pb detrital zircon sample location AXY U-Pb detrital zircon sample location; previously reported BG-1 B ^_ U-Pb crystallization sample location %, Neorchean basement age (Ma); previously reported 2582 4 F Antiform Cordierite-in isograd Synform ) Sillimanite-in isograd 3A %, M Late brittle faults ( Melt-in isograd >2556 ReL Hottah sheets - ca. 780 Ma C RXY Paleoproterozoic intrusions 64°30'N 64°30'N %,B Bishop intrusive suite - ca. 1858 to 1850 Ma 2582 'Blocky' granite; 1863 Ma P BL Zinto intrusive complex - ca. 1867 Ma XWXW Hepburn intrusive Suite - ca. 1890 Ma BL C (incudes ca. 1877 Ma sills south of 65°) Metadiorite to metagabbro A Paleoproterozoic sedimentary & volcanic rocks XW %, Snare Group quartzite and stromatolitic marble; age unknown 2582 Dumas Group volcanic and sedimentary rocks - ca. 1870 Ma IL Grant SubGroup volcanic rocks - ca. 1895 Ma; I %, may include sedimentary rocks XW Coronation sedimentary sequence; may include XW 2625 Epworth, Melville, Akaitcho, and Grant sequences XW Archean rocks - Wopmay orogen 4A M Neoarchean plutonic rocks; 2630-2575 Ma B Neoarchean metasedimentary rocks; ca. 2625 Ma ML Paleo- to Mesoarchean plutonic rocks ZL Archean rocks - Slave craton Neoarchean plutonic rocks; 2610-2575 Ma ³ Undivided Yellowknife Supergroup64°N and Central 64°N Slave Cover Group; ca. 2850-2625 Ma 116°W 115°W Unsubdivided Hadean through Neoarchean rocks 010205 Kilometers https://mc06.manuscriptcentral.com/cjes-pubs Page 47 of 80 Canadian Journal of Earth Sciences

1A B C BG-2 1270 LCL 1877 G BG-1 400 GL GL 300 ? 2820 >2900 - masl (x10) ? >2900 4020 2582 Slave craton

Schematic

2A B C W WR BWL ER

350 1893

+ 250 -

masl (x10) 1850 ? >2560 Slave craton 1850 ?

Schematic

3A R B C BLL 780 350 RL CL NL 250 >2620 2580 ? masl (x10) Slave craton 1867 1855 2580 ? 1855

Schematic 4A B <2030 780 ML ML 350 IL ML 250 02500 5000 10 000

masl (x10) ? Slave craton meters + - 1867 2582 Draft 1863 2580-2620 1855 ?

Schematic

? Relationship uncertain Gabbro dyke, sheet: Neoarchean granite, granodiorite, tonalite, Mackenzie (1270 Ma); and amphibolite; strongly deformed to Brittle fault Gunbarrel (780 Ma) gneissic, polydeformed in the Proterozoic Isograd: melt-in; sillimanite-in; cordierite/ (2620 to 2580 Ma) andalusite-in; garnet-in Coarse-grained, K-feldspar porphyritic granite (1850-1858 Ma) Neoarchean metasedimentary rocks and High strain zone minor metavolcanic rocks, polydeformed and Deformed coarse-grained, K-feldspar metamorphosed in the Archean and porphyritic granite (1863 Ma) Basement cored anticline Proterozoic (>2620 Ma) Deformed hornblende-biotite Mesoarchean granitic-amphibolitic gneiss; Unconformable surface; arrow granodiorite (1867 Ma) polydeformed (>2900 Ma) towards younging direction Deformed garnet-bearing granite Slave craton: composite Archean rocks; not W dyke (1877 Ma) Detrital zircon sample location ductiley deformed in the Proterozoic BG-1 Snare Group quartzite and stramotolitic (>2565 Ma) U-Pb zircon sample location marble; gently upright folded (age unknown) U-Pb zircon sample location; previously reported Metagabbro and diorite sills (Archean basement only) Grant Subgroup: metamorphosed basalt and lesser rhyolite (ca. 1893 Ma) Coronation metasedimentary sequence: quartz arenite, marble, calc-silicate, amphibolite, siltstone; metamorphosed and Figure 4B polydeformed (<2030 and <1920 Ma)

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116°30'W 116°15'W 116°0'W

U-Pb detrital zircon sample location M XY

F ^_ U-Pb zircon sample location F BG-2 F ^_ )" U-Pb zircon sample location (Hildebrand et al. 1990) Turmoil Lake F Unconformity

M M Late brittle faults Wopmay F Anticline

Lake Bent Lake M M Syncline

Exmouth 4 Isograd: Cordierite-in (pendante on high-grade side) Lake Paleoproterozoic intrusions Bishop intrusive suite; Black Lichen granite and BG-1 65°0'N 65°0'N Rodrigues granite ca. 1858 to 1850 Ma ^_ Zinto intrusive complex; Rebesca granodiorite )" ca. 1867 Ma M Draft Metadiorite to metagabbro

)" Granite ca. 1877 Ma Paleoproterozoic sedimentary & volcanic rocks F F Grant Subgroup volcanic rocks; basalt ca. 1895 Ma

Grant F Coronation sedimentary sequence Lake Siltstone, pelite, psammite, marble, quartz arenite;

F greenschist to amphibolite facies; <2030 Ma F Archean rocks Acasta River

F Strongly deformed to gneissic Neoarchean granite and granodiorite;

F ca. 2582 Ma; includes highly strained Proterozoic amphibolite

F F F LO XY Archean migmatic rocks of sedimentary provenance G M Gneissic Mesoarchean granite, granodiorite, and amphibolite 4 F >2950 Ma; includes highly strained Proterozoic amphibolite

4 4 F

Little4

4 4 Crapeau 4 05102.5 Lake Kilometers

4 4 4

F W XYVJ ³ 64°45'N 64°45'N

116°30'W 116°15'W 116°0'W

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116°30'W 116°20'W

60 55 j 64°35'N

64°35'N 50 S 70 j

50 S j ? ? 44

S 19

47 75 65 H S j ? 41 63

70 10 j 80 %, ? j S

D 35 37 H

? 11

37 H 1868 Ma j

S 35

S 45

68 H

17 ? 53 ! 77 34 F S

67 35

j 20 S Rebesca S 80

55 j 2 3 55 36 40 48 j Lake H S j 60 ! S

S j 83 S 70 30 S

56 S

S 60 F

j S

F !

j S 25 !

80 50 65 ! 52

48 S

S ! XY 37

j 5 j j ! R H

25 70 S 33

80 24 22 75 75 S 45 45

? F ? 46 54

S ? S 70 ? 80 ! 80 3

10 S 74 50 65 !

90 24 S 3 ! 65 38

25 ! S !

j S 64°30'N 58 S 64°30'N 3 ! 28 40

68 25 45 36 49 j

j S

40 65 ! H F S

30 25 41

65 !

j j S S ? 52 23 25 56

H ! j S 45 Draft

35 40 43 S F S 70 j %, H 53

S 2582 Ma S

S j j 80

71 55 S j 80

75 1857 Ma%, Black S S Lichen 75 Lake ³ 116°30'W 116°20'W 02.551.25 Hottah sheets - ca. 780 Ma Kilometers Paleoproterozoic intrusions Bishop intrusive suite; Black Lichen granite and Rodrigues granite ca. 1858 to 1850 Ma XY U-Pb detrital zircon sample location Zinto intrusive complex; Rebesca granodiorite %, U-Pb zircon crystallization age; previously reported ca. 1867 Ma F Unconformity; arrow points to younging direction Metadiorite to metagabbro Late brittle faults Paleoproterozoic sedimentary & volcanic rocks ! Bedding: Younging direction unknown Grant Subgroup volcanic rocks; basalt ca. 1895 Ma D Pillow flattening: Younging direction unknown Coronation sedimentary sequence Pillow basalt (unknown relationship to j Foliation Grant Subgroup) Marble and calc-silicate ? Migmatitic layering Quartz arenite S Gneissic layering Siltstone, pelite, psammite; amphibolite facies H Mineral Lineation Migmatitic sedimentary and minor volcanic rocks ! Fold Hinge: Main/unknown generation Archean rocks Strongly deformed to gneissic Neoarchean granite 3 Fold Hinge: 2nd generation and granodiorite ca. 2582 Ma; includes highly strained Proterozoic amphibolite

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S0 A

F2 S0

F1 Sgn

? F Fold F 1 B 1 Sgn cover

cover basement basement s0 S Draft gn Sgn Basement deformation F2 C prior to sedimentation F2 cover

Sgn basement

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Hottah sill (780 Ma)

Draft

A Sgn

Figure 8

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ABdata-point error ellipses are 2s data-point error ellipses are 2s BG-1 BG-1 0.498 (11dm7247a) 0.52 (11dm7247a) CA-ID-TIMS zircon 2600 SHRIMP zircon 2660 0.494 Average of two most Weighted Mean concordant analyses 2584.2 ± 2.9 [0.11%] Ma 2620 2580 0.50 2582 ± 1.1 Ma 95% conf Intercepts at 2580 0.490 2114±790 &

Pb/ U 2602±71 [±75] Ma Pb/ U 2540

206 238 2560 0.48 206 238 MSWD = 8.1 2500 0.486 Intercepts at 2460 . 2540 1870±25 & 0.46 Weighed by data point errors only 0.482 2589±10 [±20] Ma 5 of 27 rejected MSWD = 8.3 MSWD = 1.7, probability = 0.019 207Pb/ 235 U 207Pb/ 235 U 0.478 0.44 10.9 11.1 11.3 11.5 11.7 11.9 12.1 10.0 10.4 10.8 11.2 11.6 12.0 12.4 12.8

data-point error ellipses are 2s. data-point error ellipses are 2s CDBG-2 BG-2 0.346 2580 1910 (11lo4103) 0.492 (11lo4103) ID-TIMS monazite CA-ID-TIMS zircon 0.344 M1B 2570 1900 2400 0.342 } 5.7 1890 0.488 2560 2300 M1A Weighted Mean 0.340 of three most 1880 Pb/ U Draft 5.6 2200 2550 concordant analyses 0.338 206 238 2578.1 ± 1.0 Ma 1870 0.484 M1C 2100 Intercepts at Intercepts at 0.336 1874.8±1.5 Ma 5.5 1862±5 & 1168±200 & 2000 2582±10 Ma 2581.8±2.1 [±10] Ma 0.334 5.2 5.3 5.4 MSWD = 0.65 MSWD = 0.73 0.35 0.480 1900

0.33 1800 207 235

207 235 Pb/ U Pb/ U Pb/ U 0.31

206 238 0.476 45678910 11.2 11.3 11.4 11.5 11.6 11.7 E data-point error ellipses are 2s HIS-1 1930 (11lo4161) 1920 CA-ID-TIMS zircon 0.346 1910

1900 0.342

Pb/ U 1890 caption

206 238 1880 Intercepts at 0.338 301±220 & 1870 1892.4±1.9 [±6.8] Ma MSWD = 1.14

0.334

207Pb/ 235 U 0.330 5.25 5.35 5.45 5.55 5.65 5.75

Figure 9

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A10

5 depleted mantle

southwest T Slave craton

Nd 0

-5

-10 1800 2000 2200 2400 2600 AGE (Ma) 10 Bishop and Hepburn B intrusive suites (after 8 Bowring and Podosek 6 1989) Rodrigues, Peri, Black 4 Lichen K-feldspar 2 porphyritic granite T Draft 0 K-feldspar porphyritic

Nd granite e -2 Zinto suite granodiorite -4 Reworked Archean -6 granite in Wopmay -8 orogen -10 1840 1850 1860 1870 1880 1890 1900 AGE (Ma)

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A 0.008 G 2.59 7 Grant Lake quartzi arenite (11lo4166) 2.67 0.006 n=58/63 6 95-105% conc. 5 0.004 4 3

Probability 0.002 2 2.03 1 0.000 0

2750 2250 2350 2450 1850 1950 2550 2650 2050 2150 2.89 Age (Ma) B 8 0.012 R 2.6 Rebesca Lake quartz arenite (11lo4050) 7 n=43/48 95-105% conc. 6 0.008 Max. 2030 ± 16 Ma 5 2.58 4 2.03 2.66

Probability 3 0.004 2.7 2 1 0.000 0

1850 1950 2050 2150 2250 2350 2450 2550 2650 Draft2750 2.89 Age (Ma) 3.2 C 0.025 W 20 1.97 Wopmay River psammite() 11vj9205 n=81/86 18 95-105% conc.

0.020 16 Max. 1920 ± 11 Ma 14

0.015 12

initial rift

Frequency

Probability 0.010 8

2.33 6 2.6 0.005 4 1.93 2.58 2.72 2

0.000 0

1850 1950 2050 2150 2250 2350 2450 2550 2650 2750

Age (Ma)

Figure 11

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Hottah terrane Metamorphic internal zone Slave

a) a) detrital zircon detrital zircon ent craton HLMC ZF CBF TLG P-v R P-q A I M igneous igneous W G igneous n=43 Age (M Age (M n=77 n=51 n=170 n=96 ppvv n=81 n=46 n=58 n=85 n=74 n=90 n=326 n=268 Great Bear Basem 1850 Calderian arc 1850 1886 8 orogeny 1900 11 ± R Hottah rift 1906 1 ± B G Akaitcho rift 1900 1951 15 ± 1900 Hottah arc ± O ± 1920 11 Passive Taltson/ margin Ksituan? 200 0 200 0 M Initial rift ± ± ± 2030 16 2060 27 2030 16 ± 2088 14 210 0 210 0

220 0 220 0

230 0 Draft 230 0 Arrowsmith? fault zone Wopmay

240 0 240 0

Queen Maud/ Buffalo Head? 250 0 250 0

Slave/Rae? granite bloom 260 0 260 0

volcanic 270 0 270 0 belts

2080 2080 Younging Younging Basal quartz arenite/quartzite

n = number of detrital zircons 1951± 15 = maximum deposition age (Ma,±2s ) (95%-105% concordant) O = oldest bedrock in Hottah terrane (Ootes et al. 2015) v = volcanic rocks M & R = Melville Group rift sequence and Recluse Group foredeep sequence (Hoffman et al. 2011) p = plutonic rocks B & G = Bloom Basalt and Grant/Akaitcho correlation (Ootes et al. 2015)

HLMC = Holly Lake metamorphic complex psammite (Davis et al. 2015) W = Wopmay River psammite (this study) A = Arm Lake pelite (Bennett et al. 2012) ZF = Zebulon Formation quartzite (Davis et al. 2015) G = Grant Lake quartz arenite (this study) I = Ingray Lake quartzite (Bennett et al. 2012) CBF = Conjuror Bay Formation quartzite (3 samples; Davis et al. 2015) R = Rebesca Lake quartz arenite (this study) M = Mattberry Lake quartzite (5 samples; Bennett et al. 2012) TLG = Treasure Lake Group clastic sedimentary rocks (2 samples; P-v = Portage Lake volcaniclastic (Bennett et al. 2012) Bennett and Rivers 2006b; Gandhi and van Breement 2005) https://mc06.manuscriptcentral.com/cjes-pubsP-q = Portage Lake quartzite (Bennett et al. 2012) Canadian Journal of Earth Sciences Page 56 of 80

Western limit of

Diamond Mine on-craton kimberlite

WFZ Kimberlite

B Nd 0 crust 400⁰ C 40 lithospheric mantle 900⁰ C Draft

Depth (km) 80 1200⁰ C asthenosphere 0 80 160 220 300 380 Distance (km)

Figure 13

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A ca. 2020 Ma Slave initial rift Melville Group Craton

B Archean basement ca. 1970 Ma Epworth Group passive margine

C <1920 to 1890 Ma Grant Subgroup/ rift margin second rift Akaitcho Group

Hepburn intrusive Suite (ca. 1892 Ma) D ca. 1880-1860 Ma rigid backstop imbrication of rifted margin

Zinto intrusive Suite Bishop intrusive suite (ca. 1867 to 1863 Ma) (ca. 1858Draft to 1850 Ma)

Figure 14

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Table 1. TIMS U-Pb zircon and monazite results Correlation # gr Size Wt. U Pbr2 206Pb/ Pbc2 208Pb/ 207Pb/ 206Pb/ 207Pb/ 207Pb/ Discord Coefficient Fraction Description (%) (g) (ppm) (ppm) 204Pb (pg) 206Pb 235U ± 238U ± 206Pb ± 206Pb ± Bent gneiss tonalite, BG-1 #11dm7247a (lab#Z10549) *544288m E, 7221418m N A16-1 (Z) Z,Co,Clr,Eu,St,Lch,Dia1 96 1.3 114 59 5468.5 0.64 0.05 11.680 0.024 0.49078 0.00093 0.9649 0.17260 0.00009 2583.0 1.8 0.42 A16-3 (Z) Z,Co,Clr,El,Pr,Lch,Dia1 216 5 117 58 6711.5 2.62 0.04 11.313 0.013 0.48236 0.00044 0.9375 0.17009 0.00007 2558.6 1.5 0.99 A16-4 (Z) Z,Co,Clr,Eq,Pr,Lch,Dia1 241 5.9 139 70 6924.8 3.62 0.03 11.529 0.013 0.48830 0.00043 0.9352 0.17124 0.00008 2569.8 1.5 0.31 B16-1 (Z) Z,Co,Clr,Eu,Pr,Tip,Lch,Dia1 192 7.1 77 42 13099.3 1.28 0.12 11.640 0.014 0.48959 0.00045 0.9447 0.17243 0.00007 2581.4 1.4 0.59 C16-1 (Z) Z,Co,Clr,Pr,Lch,Dia 1 163 1.8 173 89 6119.7 1.55 0.05 11.482 0.014 0.48650 0.00049 0.9048 0.17117 0.00009 2569.2 1.7 0.64 Bent gneiss granite, BG-2 #11LO4103a (Z10552) *544288m E, 7221418m N A16-1 (Z) Z,Co,Clr,Pr,Sro,Lch,Dia1 146 2 164 89 2565.7 3.92 0.12 11.635 0.014 0.49035 0.00046 0.9151 0.17209 0.00009 2578.1 1.7 0.28 A16-2 (Z) Z,Co,Clr,fFr,Pr,Sub,Lch,NM10°1 230 4 95 52 5324.7 2.17 0.15 11.556 0.014 0.48775 0.00045 0.9402 0.17184 0.00008 2575.6 1.5 0.69 A16-3 (Z) Z,Co,Clr,Pr,Sub,Lch,NM10°1 140 1.5 183 101 4175.2 2.01 0.14 11.598 0.014 0.48886 0.00047 0.9292 0.17207 0.00008 2577.9 1.6 0.57 A16-4 (Z) Z,Co,Clr,fFr,Eu,Pr,Lch,NM10°1 170 1.9 144 72 1121.3 7.37 0.04 11.323 0.016 0.48058 0.00047 0.8500 0.17087 0.00013 2566.2 2.6 1.72 A16-5 (Z) Z,Co,Clr,fFr,Eu,Pr,Lch,NM10°1 200 1.9 125 68 2478.2 2.93 0.13 11.614 0.015 0.48944 0.00049 0.9238 0.17210 0.00009 2578.2 1.7 0.47 M1A (M) M,pY,Clr,Sub,NAbr,M-0.2A1 200 10 5904 6603 116997 13.81 1.78 9.560 0.014 0.44002 0.00055 0.9623 0.15758 0.00006 2429.8 1.4 3.88 M1B (M) M,pY,Clr,Sub,NAbr,M-0.2A1 100 10 3045 2538 133473 4.88 1.68 5.639 0.007 0.34409 0.00035 0.9529 0.11885 0.00005 1939.0 1.5 1.95 M1C (M) M,pY,Clr,Sub,NAbr,M-0.2A1 75 5 4277 2816 117232 3.82 1.15 5.322 0.007 0.33657 0.00035 0.9540 0.11468 0.00005 1874.8 1.5 0.29 Hepburn intrusive suite, HIS-1 #11LO4161a (Z10557) Draft *537558m E, 7296798m N A10-1 (Z) Z,Co,Clr,Eu,Pr,Lch,NM10°1 125 1.3 219 81 6600.5 0.92 0.15 5.427 0.007 0.33985 0.00036 0.9331 0.11581 0.00006 1892.5 1.7 0.4 A10-2 (Z) Z,Co,Clr,Eu,Pr,Lch,NM10°1 80 0.8 103 40 423.1 4.29 0.22 5.455 0.016 0.34145 0.00052 0.6600 0.11587 0.00026 1893.4 8.0 -0.01 A10-3 (Z) Z,Co,Clr,fIn,Eu,Pr,Lch,NM10°1 230 3.7 118 44 2474.5 3.83 0.14 5.634 0.007 0.34620 0.00034 0.8501 0.11803 0.00008 1926.6 2.4 0.61 B10-1 (Z) Z,pBr,Tb,nFr,Eu,St,Lch,M10°1 260 15.3 99 36 9169.6 3.48 0.15 5.393 0.006 0.33820 0.00029 0.9418 0.11565 0.00005 1890.0 1.6 0.73 B5-1 (Z) Z,pBr,Tb,nFr,Eu,Pr,Lch,M10°1 165 3 191 70 5931.5 2.02 0.15 5.346 0.006 0.33529 0.00031 0.9301 0.11565 0.00005 1890.0 1.7 1.59 B5-2 (Z) Z,pBr,Tb,nFr,Eu,Pr,Lch,M10°1 157 2.5 206 75 9350 0.75 0.14 5.335 0.006 0.33473 0.00033 0.9105 0.11560 0.00006 1889.2 1.8 1.7 B5-3 (Z) Z,pBr,Tb,nFr,Eu,Pr,Lch,M10°1 121 1.3 118 44 2035.6 1.59 0.18 5.375 0.014 0.33638 0.00091 0.8231 0.11589 0.00018 1893.7 5.6 1.49

*UTM Zone 11, NAD 83 Z=Zircon, M=Monazite, Co=Colourless, pBr=Pale Brown, pY=Pale Yellow, Clr=Clear, Tb=Turbid, fFr=Few Fractures, nFr=Numerous Fractures, fIn=Few Inclusions, El=Elongate, Eq=Equant, Eu=Euhedral, Pr=Prismatic Sro=Subrounded, St=Stubby Prism, Sub=Subhedral, Tip=Tip, NAbr=Not Abraded, Lch=Leached (1) Weights estimated Concentration uncertainty up to 50% (2) Pbr = radiogenic Pb. Pbc = total common Pb in analysis corrected for spike and fractionation. (3) Atomic ratios corrected for spike, fractionation, blank and initial common Pb, except 206Pb/204Pb ratio corrected for spike and fractionation only. Errors are one sigma absolute. Pb blank:1-2 pg for zircon ; blank composition in atomic proportions = 51.966:21.356:25.288:1.3895 (208:207:206:204)

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10549-1.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-2.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-3.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-4.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-8.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-6.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-5.1 627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-11.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-12.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-10.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-15.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-14.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-16.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-24.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-21.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-18.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 10549-17.1627 627_1_2012_Jan_30_11.45PDF 6266 Zircon 0 0 Draft

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46.65 233.7584 68.97956 0.304827 0.118037 456.2287 1.65111 10741.83 29.15967 46.933 259.6453 51.97278 0.206774 0.415992 369.7801 1.296704 10964.65 27.34035 47.217 180.2606 29.69801 0.170187 0.288199 281.0356 1.141316 11201.85 55.34436 47.8 170.1058 69.83951 0.424114 0.375754 341.6812 1.309764 10291.87 27.46557 48.083 207.4717 82.09544 0.408753 0.202381 242.3285 0.983255 10986.2 66.97999 48.383 305.8519 20.07622 0.067806 0.333404 63.38027 0.435653 12279.89 31.80659 48.95 139.9315 79.60512 0.58766 0.032771 266.0428 1.081546 10324.96 27.26356 49.25 321.2966 20.75564 0.066731 0.606991 474.0891 1.963598 12517.24 31.67896 49.533 215.1361 21.99353 0.105604 0.380635 322.6613 1.276454 11870.23 31.99141 49.817 217.3689 17.00994 0.080836 0.293137 100.0074 0.549249 12419.75 30.85305 50.1 244.3965 37.898 0.160185 0.459384 170.782 0.818551 11672.03 31.21794 50.4 187.435 36.4629 0.200956 0.456965 260.9518 1.054945 12427.72 32.13494 50.683 140.9342 53.35997 0.391111 0.496498 211.0521 0.972428 10281.29 28.31596 51.25 381.6341 19.30089 0.052243 0.528549 473.5724 1.622504 12890.71 55.73856 51.55 210.5185 8.573097 0.042068 0.236935 34.36665 0.317041 12371.37 32.42964 51.833 221.0513 12.73077 0.059492 0.82301 41.65619 1.502088 12286.26 31.05629 52.117 221.6255 100.0532 0.46635 0.300083 353.6978 2.18969 10605.84 48.27346 Draft

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2.09E-05 81.73446 0.036301 98.54661 0.085157 1.629863 11.70868 1.142528 0.490774 5.69E-06 216.881 0.00986 108.5456 0.055911 1.740916 11.5594 1.142428 0.486675 2.02E-05 28.14885 0.035084 75.88393 0.048405 2.786839 11.64681 1.168281 0.490067 1.24E-05 48.34645 0.021506 71.32867 0.124995 1.549854 11.63537 1.220358 0.488148 2.57E-06 140.881 0.00445 87.71126 0.120079 1.372602 11.81551 1.502953 0.492157 1.3E-05 29.76466 0.022471 127.8178 0.01797 2.917816 11.55028 1.570554 0.486505 2.16E-05 33.0286 0.03752 56.53447 0.169544 2.504035 10.96913 1.158738 0.470332 2.57E-06 97.10942 0.004458 135.6508 0.019453 2.689789 11.73134 1.144968 0.491499 4.03E-05 32.59034 0.069794 91.8325 0.024855 2.924543 11.76626 1.140817 0.496924 -8.7E-06 65.02786 -0.01505 90.68463 0.021795 3.107283 11.5182 1.440893 0.485672 2.89E-06 368.5976 0.005005 103.4644 0.04182 2.236197 11.58476 1.461915 0.492836 4.49E-05 37.32984 0.077765 78.35357 0.056235 2.136822 11.43364 1.14871 0.486648 2.65E-05 21.25397 0.045942 60.44269 0.106359 1.910559 11.91702 1.235255 0.499269 6.26E-06 198.4966 0.010843 162.3962 0.014479 2.915497 11.85347 1.123405 0.495377 -4.3E-06 67.99643 -0.00744 90.27385 0.013301 4.116077 11.79695 3.284757 0.499205 2.59E-05 36.63164 0.044856 99.54098 0.016 4.993366 12.25446 4.041563 0.524223 3.35E-05 49.14713 0.058126 94.52835 0.1357 1.304124 11.79044 1.143428 0.496534 Draft

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1.113059 0.974208 0.173032 0.257816 2574.023 23.62142 2587.185 4.302764 0.617011 1.121597 0.981766 0.172264 0.217166 2556.273 23.66889 2579.765 3.626964 1.102951 1.13947 0.975339 0.172365 0.257852 2570.967 24.15856 2580.745 4.306065 0.459375 1.191572 0.976411 0.172873 0.263498 2562.66 25.19672 2585.653 4.398244 1.07757 1.174993 0.78179 0.17412 0.937154 2579.999 24.98288 2597.642 15.62462 0.824049 1.365135 0.869206 0.172189 0.77656 2555.536 28.80147 2579.03 12.97051 1.103282 1.120476 0.96698 0.169148 0.295308 2485.018 23.10521 2549.227 4.946764 3.034376 1.130485 0.987351 0.17311 0.181535 2577.16 24.01501 2587.945 3.029476 0.505559 1.11388 0.976388 0.17173 0.246445 2600.563 23.83673 2574.579 4.118031 -1.22667 1.348987 0.936216 0.172005 0.506366 2551.924 28.42799 2577.246 8.459058 1.189671 1.310723 0.896579 0.170484 0.647457 2582.936 27.89457 2562.398 10.8317 -0.97289 1.115222 0.970848 0.170399 0.275343 2556.157 23.5335 2561.57 4.606753 0.255937 1.198157 0.969967 0.173114 0.300458 2610.652 25.72093 2587.979 5.014044 -1.06559 1.106886 0.985296 0.173544 0.19194 2593.896 23.63775 2592.115 3.201819 -0.08348 2.435445 0.741438 0.171392 2.204141 2610.377 52.27744 2571.28 36.84246 -1.84948 2.959158 0.732182 0.169542 2.752746 2717.064 65.60754 2553.126 46.09416 -7.87606 1.113747 0.974042 0.172218 0.258836 2598.884 23.8214 2579.32 4.323098 -0.92175 Draft

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17.334 0.895 2.1384 2.036859 1.112663 17.334 0.895 2.1384 2.054558 1.121393 17.334 0.895 2.1384 2.03982 1.139428 17.334 0.895 2.1384 2.048117 1.191526 17.334 0.895 2.1384 2.031783 1.174977 17.334 0.895 2.1384 2.055016 1.365119 17.334 0.895 2.1384 2.125359 1.120407 17.334 0.895 2.1384 2.0345 1.130476 17.334 0.895 2.1384 2.010975 1.113647 17.334 0.895 2.1384 2.059313 1.348952 17.334 0.895 2.1384 2.028969 1.310593 17.334 0.895 2.1384 2.053275 1.114844 17.334 0.895 2.1384 2.002009 1.198117 17.334 0.895 2.1384 2.018447 1.106677 17.334 0.895 2.1384 2.003336 2.43544 17.334 0.895 2.1384 1.906731 2.959113 17.334 0.895 2.1384 2.012789 1.11338 Draft

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0.172776 0.225445 2570.494 33.74391 0.137103 0.17182 0.197512 2548.49 33.402 0.131595 0.172104 0.254015 2568.916 34.51943 0.139386 0.172511 0.259575 2555.007 35.6934 0.143867 0.173631 0.936577 2574.472 36.35843 0.144581 0.171836 0.77514 2547.762 40.97044 0.128929 0.168914 0.289863 2462.547 31.25744 0.135694 0.172625 0.180587 2574.647 34.38476 0.143277 0.171722 0.226059 2614.438 35.02301 0.116956 0.171381 0.505078 2543.427 40.14044 0.130945 0.17001 0.642487 2594.056 40.7406 0.128666 0.170454 0.244838 2555.99 33.42203 0.136183 0.172928 0.296955 2623.264 37.9847 0.135771 0.173103 0.169531 2596.914 34.28084 0.137288 0.170825 2.204896 2630.393 79.29514 0.157836 0.16936 2.745318 2807.741 113.8891 0.140989 0.172124 0.228432 2609.869 34.88142 0.144483 Draft

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2.112804 2596.938 51.48962 2.265031 2498.794 53.2397 3.055864 2637.475 75.56056 1.998656 2716.821 50.80872 1.821545 2729.427 46.50697 3.334993 2451.133 76.98293 2.747913 2571.883 66.36154 3.017928 2706.399 76.44502 3.711207 2235.619 78.54458 3.532995 2487.183 82.68066 2.796287 2446.411 64.4308 2.690381 2580.587 65.17829 2.3175 2573.254 55.99513 4.484649 2600.232 109.422 4.857076 2962.158 133.8284 6.260526 2665.899 156.361 1.798136 2727.706 45.88228 Draft

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1.003 25166.34 6.140386 0.216584 1.003 29595.64 6.181954 0.189736 1.003 25829.14 6.145249 0.241553 1.003 26179.42 6.175209 0.246048 1.003 28337.86 6.124656 0.2155 1.003 27649.66 6.133283 0.181152 1.003 26884.77 6.134507 0.267136 1.003 28398.92 6.169606 0.174951 1.003 25098.63 6.320712 0.22281 1.003 29840.66 6.130136 0.204494 1.003 25764.75 6.151676 0.211003 1.003 27011.83 6.14687 0.230207 1.003 24033.75 6.125944 0.485442 1.003 27446.4 6.169983 0.16637 1.003 26395.76 6.226832 0.216491 1.003 28023.54 6.156453 0.209605 1.003 24520.98 6.236813 0.219094 Draft

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Table 2. SHRIMP II U-Pb zircon results. Atomic Ratios Model Age (Ma) Spot name U Th Th Yb Hf 204Pb ± 204Pb 206Pb* 208*Pb ± 208Pb 207*Pb ±207Pb 206*Pb ±206Pb Corr 207*Pb ±207Pb 206Pb ±206Pb 207Pb ±207Pb Disc. 206 206 204 206* 206 235 235 238 238 206* 206 238 238 206 206 (ppm) (ppm) U (ppm) (ppm) Pb Pb f(206) (ppm) Pb Pb U U U U Coeff Pb Pb U U Pb Pb (%) Bent gneiss tonalite, BG-1 (#11dm7247a) *544288m E, 7221418m N 10549-1.1 234 69 0.30 456 10742 2.1E-5 82 0.04 98.5 0.085 1.6 11.71 1.1 0.4908 1.1 0.974 0.1730 0.3 2574 24 2587 4 +1 10549-2.1 260 52 0.21 370 10965 5.7E-6 217 0.01 108.5 0.056 1.7 11.56 1.1 0.4867 1.1 0.982 0.1723 0.2 2556 24 2580 4 +1 10549-3.1 180 30 0.17 281 11202 2.0E-5 28 0.04 75.9 0.048 2.8 11.65 1.2 0.4901 1.1 0.975 0.1724 0.3 2571 24 2581 4 +0 10549-4.1 170 70 0.42 342 10292 1.2E-5 48 0.02 71.3 0.125 1.5 11.64 1.2 0.4881 1.2 0.976 0.1729 0.3 2563 25 2586 4 +1 10549-8.1 207 82 0.41 242 10986 2.6E-6 141 0.00 87.7 0.120 1.4 11.82 1.5 0.4922 1.2 0.782 0.1741 0.9 2580 25 2598 16 +1 10549-6.1 306 20 0.07 63 12280 1.3E-5 30 0.02 127.8 0.018 2.9 11.55 1.6 0.4865 1.4 0.869 0.1722 0.8 2556 29 2579 13 +1 10549-5.1 140 80 0.59 266 10325 2.2E-5 33 0.04 56.5 0.170 2.5 10.97 1.2 0.4703 1.1 0.967 0.1691 0.3 2485 23 2549 5 +3 10549-11.1 321 21 0.07 474 12517 2.6E-6 97 0.00 135.7 0.019 2.7 11.73 1.1 0.4915 1.1 0.987 0.1731 0.2 2577 24 2588 3 +1 10549-12.1 215 22 0.11 323 11870 4.0E-5 33 0.07 91.8 0.025 2.9 11.77 1.1 0.4969 1.1 0.976 0.1717 0.2 2601 24 2575 4 -1 10549-10.1 217 17 0.08 100 12420 --8.7E-6 65 -0.02 90.7 0.022 3.1 11.52 1.4 0.4857 1.3 0.936 0.1720 0.5 2552 28 2577 8 +1 10549-15.1 244 38 0.16 171 11672 2.9E-6 369 0.01 103.5 0.042 2.2 11.58 1.5 0.4928 1.3 0.897 0.1705 0.6 2583 28 2562 11 -1 10549-14.1 187 36 0.20 261 12428 4.5E-5 37 0.08 78.4 0.056 2.1 11.43 1.1 0.4866 1.1 0.971 0.1704 0.3 2556 24 2562 5 +0 10549-16.1 141 53 0.39 211 10281 2.7E-5 21 0.05 60.4 0.106 1.9 11.92 1.2 0.4993 1.2 0.970 0.1731 0.3 2611 26 2588 5 -1 10549-24.1 382 19 0.05 474 12891 6.3E-6 198 0.01 162.4 0.014 2.9 11.85 1.1 0.4954 1.1 0.985 0.1735 0.2 2594 24 2592 3 -0 10549-21.1 211 9 0.04 34 12371 --4.3E-6 68 -0.01 90.3 0.013 4.1 11.80 3.3 0.4992 2.4 0.741 0.1714 2.2 2610 52 2571 37 -2 10549-18.1 221 13 0.06 42 12286 2.6E-5 37 0.04 99.5 0.016 5.0 12.25 4.0 0.5242 3.0 0.732 0.1695 2.8 2717 66 2553 46 -8 10549-17.1 222 100 0.47 354 10606 3.4E-5 49 0.06 94.5 0.136 1.3 11.79 1.1 0.4965 1.1 0.974 0.1722 0.3 2599 24 2579 4 -1

*UTM Zone 11, NAD 83 Spot name follows the convention x-y.z; where x = sample number, y = grain number and z = spot number. Multiple analyses in an individual spot are labelled as x-y.z.z Uncertainties reported at 1s% and are calculated by numerical propagation of all known sources of error using Squid version 2.22. Errors in ages are 1s absolute in Ma. f206204 refers to mole fraction of total 206Pb that is due to common Pb, calculated using the 204Pb-method; common Pb Draftcomposition used is the surface blank (4/6: 0.05770; 7/6: 0.89500; 8/6: 2.13840) * refers to radiogenic Pb (corrected for common Pb) Discordance relative to origin = 100 * (1-(206Pb/238U age)/(207Pb/206Pb age)) Calibration standard 6266; U = 910 ppm; Age = 559 Ma; 206Pb/238U = 0.09059 Th/U calibration: F = 0.03900*UO + 0.85600

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Table 3. Sm-Nd isotope results. 143 144 Nd/ Nd 147 144 143 144 uncertainty +/- T TDM (Ga) Unit Age (Ma) Sample# UTM X UTM Y Lab-year Nd (ppm) Total Sm Sm/ Nd Nd/ Nd(i) εNd CHUR (est) (2σ) (0.214, 0.513115) Black Lichen - Bishop 1855 06vj218 538465 7145650 UBC-08 54.9 0.511218 9.57 0.105349 0.509932 0.000008 -6.0 2.66 Black Lichen - Bishop 1855 06vj219 538391 7139488 UBC-08 83.8 0.511075 12.75 0.091948 0.509953 0.000006 -5.6 2.55 Black Lichen - Bishop 1855 06vj220 531800 7139645 UBC-08 68.9 0.511228 12.1 0.106135 0.509933 0.000006 -6.0 2.66 Black Lichen - Bishop 1855 06vj139A 533652 7146374 UBC-08 96.2 0.511090 14.6 0.091719 0.509971 0.000008 -5.2 2.52 Rodrigues - Bishop 1855 10lo1054a 546416 7180396 Carleton-12 50.5 0.511301 9.13 0.109316 0.509970 0.000017 -5.4 2.63 Peri Granite - Bishop 1858 04-WOP-3201 525243 7110433 Carleton-05 54.8 0.511218 10.0 0.110661 0.509865 *0.000018 -7.2 2.78 Peri Granite - Bishop 1858 04-WOP-3375B 528688 7117764 Carleton-05 52.2 0.511276 10.1 0.116873 0.509848 *0.000019 -7.6 2.86 Phenocrystic granite 1863 06vj216 518472 7141573 UBC-08 45.3 0.511311 8.09 0.107933 0.509986 0.000009 -4.7 2.59 Phencrystic granite 1863 04-WOP-3004 518258 7111640 Carleton-05 41.4 0.511320 7.3 0.106262 0.510018 *0.000018 -4.1 2.53 Phencrystic granite 1863 04-WOP-3018 519276 7115548 Carleton-05 104.3 0.511349 18.9 0.109289 0.510010 *0.000018 -4.3 2.56 Zinto 1867 06vj215 516652 7139953 UBC-08 40.7 0.511261 6.76 0.100381 0.510029 0.000007 -3.8 2.49 Zinto 1867 04-WOP-3187 523774 7102185 Carleton-05 42.2 0.511295 7.3 0.104931 0.510006 *0.000018 -4.2 2.53 Zinto 1867 04-WOP-3239 524251 7098915 Carleton-05 41.1 0.511315 7.2 0.106551 0.510005 *0.000018 -4.2 2.54 Zinto 1867 04-WOP-3114 531749 7098714 Carleton-05 46.7 0.511244 7.9 0.101910 0.509992 *0.000017 -4.5 2.53 Zinto 1867 11mh8019a 524505 7160446.1 Carleton-12 40.9 0.511400 7.5 0.110186 0.510044 0.000033 -3.4 2.51 Zinto 1867 11lo4181a 551627.49 7203501.1 Carleton-12 80.0 0.511229 13.3 0.100676 0.509990 0.000031 -4.5 2.52 Mattberry granite 2582 04-WOP-0129A 520548 7108356 Carleton-05 59.8 0.511360 12.2 0.122953 0.509268 *0.000024 -0.5 2.92 Bent granite 2582 11lo4103a 544288.33 7221418.7 Carleton-12 32.7 0.511225 6.2 0.114495 0.509277 0.000037 -0.3 2.88 Rebesca gneiss 2582 11lo4006a 533379.35 7153051 Carleton-12Draft 26.6 0.512665 8.8 0.199782 0.509266 0.000063 -0.5 - Crapeau gneiss 2582 09vj170b 521681.8 7191540.5 Carleton-12 42.5 0.511332 8.3 0.118047 0.509324 0.000038 0.6 2.82 Grant gneiss 2582 09vj174a 522884.07 7199747.8 Carleton-12 21.1 0.511198 3.8 0.109169 0.509341 0.000035 1.0 2.77 Grant gneiss 2582 09lo9028a 528468 7191518.3 Carleton-12 63.1 0.511074 10.7 0.102490 0.509330 0.000033 0.8 2.77 Rodrigues gneiss 2582 10lo1075 564322.96 7183212.9 Carleton-12 14.8 0.510801 2.1 0.086380 0.509331 0.000029 0.8 2.75 Notes: UTM Zone 11, NAD 83; UBC - University of British Columbia, 2008, following procedures in Weiss et al. (2006a,b) Carleton University 2005 and 2012 - Carelton-05 data followed procedures in Cousens (1996); Carleton-12 followed procedures in Hollings et al. (2012) 143Nd/144Nd(i) 2σ uncertainty in UBC-08 and Carleton-12 is from individual runs, 143Nd/144Nd(i) 2σ uncertainty in Carleton-05 (*) is calculated from uncertainty in age (+/- 10 Ma, 2σ) and Sm/Nd,

TDM calculated acording to Goldstein et al. (1984)

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Table 4. SHRIMP II U-Pb detrital zircon results. Spot name U Th Th Yb Hf 204Pb ± 204Pb 206Pb* 208*Pb ± 208Pb 207*Pb ±207Pb 206*Pb ±206Pb Corr 207*Pb ±207Pb 206Pb ±206Pb 207Pb ±207Pb Disc. 206 206 204 206* 206 235 235 238 238 206* 206 238 238 206 206 (ppm) (ppm) U (ppm) (ppm) Pb Pb f(206) (ppm) Pb Pb U U U U Coeff Pb Pb U U Pb Pb (%) Rebesca Lake quartz arenite, R (#11lo4050) *532316m E, 7155607m N 10561-001.1 115 100 0.89 428 8335 0.000644 21 1.12 50.1 0.254 2.2 12.61 1.7 0.5053 1.2 0.736 0.1809 1.1 2637 26 2662 19 +1 10561-002.1 161 54 0.35 183 9758 0.000749 46 1.30 64.3 0.087 4.5 11.21 3.2 0.4656 1.5 0.480 0.1746 2.8 2464 31 2602 47 +6 10561-003.1 585 95 0.17 175 12835 0.000116 17 0.20 245.2 0.048 2.3 11.58 1.2 0.4883 1.1 0.961 0.1719 0.3 2564 24 2577 5 +1 10561-008.1 281 104 0.38 213 10527 0.000283 25 0.49 115.3 0.115 3.2 11.88 1.8 0.4784 1.5 0.819 0.1801 1.0 2520 30 2653 17 +6 10561-012.1 702 62 0.09 70 10918 0.000037 29 0.06 288.9 0.025 2.9 11.38 1.1 0.4794 1.1 0.973 0.1722 0.3 2525 23 2579 4 +3 10561-013.1.2 92 37 0.42 125 9294 0.000585 26 1.01 29.0 0.112 5.6 6.21 2.5 0.3649 1.5 0.606 0.1234 2.0 2006 26 2006 35 +0 10561-015.1 201 161 0.83 259 10943 0.000574 24 1.00 82.8 0.232 3.3 11.48 1.9 0.4794 1.4 0.718 0.1737 1.3 2525 29 2594 22 +3 10561-017.1 383 185 0.50 285 10333 0.000061 43 0.11 118.7 0.153 2.3 6.24 1.3 0.3612 1.1 0.884 0.1253 0.6 1988 20 2033 11 +3 10561-019.2 185 75 0.42 337 10156 0.000026 41 0.05 77.9 0.117 3.9 11.82 1.3 0.4905 1.2 0.902 0.1749 0.6 2573 25 2605 9 +1 10561-020.1 130 49 0.39 153 9570 0.000890 23 1.54 41.3 0.115 3.6 6.32 2.8 0.3685 1.2 0.444 0.1243 2.5 2022 22 2019 45 -0 10561-021.2 146 84 0.59 284 9000 0.000064 24 0.11 64.6 0.158 3.7 12.90 1.3 0.5136 1.2 0.889 0.1821 0.6 2672 26 2672 10 +0 10561-024.1 116 52 0.46 194 9623 0.000225 122 0.39 49.1 0.128 4.0 11.83 2.6 0.4919 1.5 0.563 0.1745 2.1 2579 31 2601 36 +1 10561-025.1 244 110 0.47 230 9977 0.001001 18 1.74 75.7 0.147 3.4 6.09 2.6 0.3615 1.2 0.471 0.1223 2.3 1989 21 1990 40 +0 10561-049.1 345 182 0.54 274 8216 0.000080 27 0.14 151.3 0.154 1.7 13.03 1.2 0.5100 1.1 0.951 0.1853 0.4 2656 25 2701 6 +2 10561-054.1 111 73 0.68 118 9119 0.000417 37 0.72 45.9 0.180 2.7 11.42 1.8 0.4811 1.2 0.683 0.1722 1.3 2532 26 2579 22 +2 10561-056.1 89 61 0.71 140 9502 0.000130 31 0.22 38.3 0.204 4.1 12.44 1.5 0.4996 1.3 0.833 0.1806 0.8 2612 27 2658 14 +2 10561-057.1 92 84 0.95 259 9354 0.000225 52 0.39 36.8 0.257 3.0 11.38 1.7 0.4676 1.3 0.738 0.1764 1.2 2473 26 2620 19 +7 10561-058.1.2 18 6 0.35 99 8194 0.000481 27 0.83 8.0 0.095 12.0 13.36 2.6 0.5164 1.7 0.668 0.1876 1.9 2684 38 2721 31 +2 10561-060.1 71 41 0.60 154 11859 0.000075 159 0.13 30.0 0.169 3.7 12.28 1.7 0.4926 1.3 0.741 0.1808 1.1 2582 27 2661 19 +4 10561-061.1 98 51 0.54 156 8642 0.000758 24 1.31 41.6 0.142 4.3 11.64 2.0 0.4926 1.3 0.629 0.1714 1.6 2582 27 2572 26 -0 10561-062.1 56 35 0.65 195 9313 0.000713 22 1.24 22.9 0.185 3.7 11.73 1.9 0.4793 1.3 0.675 0.1774 1.4 2524 27 2629 24 +5 10561-064.1 182 150 0.85 428 8201 0.000041 82 0.07 95.4 0.234 2.6 21.07 1.5 0.6116 1.4 0.948 0.2498 0.5 3076 35 3184 8 +4 10561-065.1 395 219 0.57 308 12084 0.000106 19 0.18 165.4Draft 0.158 1.6 11.71 1.4 0.4882 1.4 0.967 0.1739 0.4 2563 29 2596 6 +2 10561-066.2 8 6 0.70 116 6240 0.000000 100 0.00 2.5 0.201 15.5 6.18 3.9 0.3566 2.2 0.558 0.1257 3.3 1966 37 2039 58 +4 10561-068.1 234 96 0.43 230 11179 0.000064 80 0.11 99.4 0.116 2.4 11.86 1.3 0.4942 1.1 0.894 0.1740 0.6 2589 24 2597 10 +0 10561-071.1 315 64 0.21 177 10737 0.000022 57 0.04 168.3 0.055 2.7 21.61 1.2 0.6228 1.1 0.940 0.2517 0.4 3121 28 3196 7 +3 10561-075.1 53 44 0.85 123 8965 0.000267 127 0.46 16.8 0.233 4.0 6.14 4.2 0.3670 1.4 0.336 0.1214 4.0 2015 24 1977 70 -2 10561-077.1 211 150 0.73 235 11315 0.000042 107 0.07 89.8 0.203 2.7 12.09 1.3 0.4966 1.2 0.891 0.1766 0.6 2599 25 2621 10 +1 10561-078.1 105 136 1.33 194 7635 0.000133 25 0.23 44.5 0.382 2.0 11.82 1.4 0.4938 1.2 0.868 0.1736 0.7 2587 25 2593 11 +0 10561-079.1 137 91 0.69 97 9903 0.000128 36 0.22 59.3 0.194 2.5 12.72 1.3 0.5035 1.2 0.877 0.1833 0.6 2629 26 2683 11 +2 10561-080.1 165 99 0.62 297 8532 0.000116 29 0.20 69.4 0.172 2.4 11.93 1.3 0.4894 1.2 0.901 0.1768 0.6 2568 25 2623 10 +3 10561-082.1 103 163 1.63 124 9911 0.000317 23 0.55 42.5 0.455 1.8 11.62 1.5 0.4789 1.2 0.822 0.1760 0.8 2522 25 2616 14 +4 10561-083.1 84 36 0.44 131 8345 -0.000101 31 -0.17 27.4 0.136 6.1 6.65 1.8 0.3804 1.4 0.786 0.1268 1.1 2078 24 2055 19 -1 10561-084.1 426 122 0.30 109 11779 0.000057 26 0.10 200.2 0.080 2.1 15.66 1.2 0.5470 1.1 0.963 0.2076 0.3 2813 26 2887 5 +3 10561-085.1 179 200 1.15 212 8974 0.000049 38 0.09 79.0 0.321 2.3 12.75 1.4 0.5124 1.2 0.913 0.1805 0.6 2667 27 2657 9 -0 10561-088.1 178 90 0.52 156 10214 0.000028 135 0.05 84.9 0.144 3.3 15.91 1.3 0.5561 1.2 0.907 0.2075 0.6 2850 27 2886 9 +2 10561-090.1 219 90 0.43 229 10268 0.000081 53 0.14 88.5 0.122 2.5 11.38 1.3 0.4696 1.1 0.899 0.1757 0.6 2482 24 2613 9 +6 10561-091.1 133 69 0.53 224 8551 0.000114 30 0.20 55.9 0.150 2.5 11.83 1.3 0.4904 1.2 0.902 0.1749 0.6 2572 25 2605 9 +2 10561-092.1 206 143 0.72 200 10906 0.000025 100 0.04 88.1 0.208 1.7 11.93 1.2 0.4975 1.1 0.931 0.1739 0.4 2603 24 2596 7 -0 10561-093.1 55 27 0.52 147 8774 0.000051 63 0.09 22.8 0.142 4.1 11.70 1.5 0.4856 1.3 0.830 0.1747 0.8 2552 26 2603 14 +2 10561-094.1 290 130 0.46 264 9682 0.000041 65 0.07 90.2 0.139 2.1 6.25 1.2 0.3626 1.1 0.903 0.1250 0.5 1995 19 2029 9 +2 10561-095.1 208 150 0.74 125 9716 0.000061 29 0.10 88.6 0.211 1.7 12.30 1.2 0.4949 1.1 0.939 0.1803 0.4 2592 24 2655 7 +3 10561-096.1 38 21 0.56 147 8648 0.000350 70 0.61 16.0 0.154 5.0 11.33 2.6 0.4858 1.4 0.552 0.1691 2.2 2552 30 2549 36 -0 10561-097.1 199 107 0.55 135 9794 0.000111 31 0.19 62.7 0.163 2.4 6.31 1.3 0.3659 1.1 0.858 0.1250 0.7 2010 20 2028 12 +1 10561-098.1 90 47 0.53 195 9097 0.000151 35 0.26 38.8 0.152 3.4 12.53 1.4 0.4992 1.2 0.842 0.1820 0.8 2610 26 2672 13 +3 10561-100.1 268 135 0.52 186 9554 0.000018 43 0.03 125.3 0.143 2.0 15.59 1.2 0.5453 1.1 0.949 0.2073 0.4 2805 26 2885 6 +3 10561-101.1 106 45 0.44 131 8441 0.000214 52 0.37 33.2 0.134 3.9 6.19 1.9 0.3642 1.2 0.629 0.1232 1.5 2002 21 2003 27 +0 10561-102.1 108 67 0.64 254 10155 0.000138 136 0.24 46.2 0.186 2.8 11.99 2.0 0.4978 1.3 0.660 0.1746 1.5 2604 28 2603 25 -0 10561-103.1 215 46 0.22 177 8629 0.000050 17 0.09 89.0 0.063 3.5 11.60 1.2 0.4829 1.1 0.926 0.1743 0.5 2540 24 2599 8 +3 10561-105.1 197 81 0.42 139 10260 0.000027 71 0.05 82.2 0.122 2.3 11.62 1.2 0.4846 1.1 0.930 0.1739 0.4 2547 24 2596 7 +2 10561-106.1 84 90 1.10 230 8233 0.000261 30 0.45 35.2 0.295 2.5 11.65 1.5 0.4874 1.2 0.798 0.1733 0.9 2560 26 2590 15 +1 10561-108.1 51 42 0.84 170 7399 0.000332 43 0.58 15.8 0.267 5.5 6.20 2.5 0.3604 1.4 0.546 0.1248 2.1 1984 23 2025 37 +2

Grant Lake quartz arenite, G (#11lo4166) *527929m E, 7192171m N 10562-001.1 73 41 0.58 88 8449 0.000228 19 0.40 30.5 0.155 4.8 11.42 1.8 0.4843 1.5 0.834 0.1711 1.0 2546 31 2568 16 +1 10562-002.1 83 34 0.42 242 8518 0.000091 24 0.16 38.1 0.124 4.9 13.59 1.9 0.5343 1.7 0.900 0.1844 0.8 2759 39 2693 14 -3 10562-003.1 34 38 1.15 104 8737 0.000192 37 0.33 14.6 0.294 5.1 12.46 2.4 0.4994 1.9 0.808 0.1809 1.4 2611 41 2661 23 +2

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10562-004.1 68 33 0.50 351 8620 0.000075 74 0.13 29.0 0.138 5.1 13.37 2.1 0.4961 1.9 0.891 0.1954 0.9 2597 40 2788 15 +8 10562-005.1 155 55 0.37 200 9564 -0.000040 38 -0.07 65.3 0.106 4.2 11.67 1.4 0.4904 1.3 0.890 0.1726 0.6 2572 27 2583 11 +0 10562-006.1 79 57 0.75 117 8385 0.000221 39 0.38 33.2 0.210 3.9 11.57 1.8 0.4929 1.5 0.803 0.1702 1.1 2583 31 2560 18 -1 10562-009.1 53 38 0.74 132 8601 0.000099 65 0.17 24.7 0.192 5.3 13.71 2.6 0.5387 2.4 0.895 0.1845 1.2 2778 53 2694 19 -4 10562-010.1 39 26 0.69 104 10033 0.000152 30 0.26 17.7 0.194 6.2 13.41 2.3 0.5354 1.9 0.816 0.1816 1.3 2764 42 2668 22 -4 10562-011.1 185 157 0.87 205 8885 0.000049 150 0.09 79.6 0.230 2.6 11.92 1.5 0.5004 1.2 0.839 0.1727 0.8 2615 27 2584 13 -1 10562-013.1 91 75 0.86 103 9014 0.000179 35 0.31 37.6 0.229 3.9 11.64 1.8 0.4823 1.5 0.826 0.1750 1.0 2537 31 2606 17 +3 10562-014.1 83 62 0.78 113 8958 0.000125 35 0.22 34.7 0.202 4.2 11.60 1.8 0.4895 1.5 0.837 0.1719 1.0 2568 31 2576 16 +0 10562-015.1 205 117 0.59 404 8320 0.000061 34 0.11 89.8 0.163 2.9 12.90 1.3 0.5100 1.2 0.906 0.1834 0.6 2657 26 2684 9 +1 10562-016.1 183 129 0.73 135 10377 0.000071 43 0.12 80.7 0.202 2.8 12.87 1.4 0.5132 1.2 0.892 0.1819 0.6 2670 27 2670 10 -0 10562-017.1 84 69 0.84 128 8683 0.000076 29 0.13 36.5 0.233 4.0 12.00 1.7 0.5046 1.5 0.849 0.1725 0.9 2634 32 2582 15 -2 10562-021.1 41 18 0.46 158 8604 0.000466 20 0.81 18.4 0.120 7.6 13.24 2.4 0.5238 1.9 0.798 0.1833 1.5 2715 43 2683 24 -1 10562-023.1 109 65 0.62 99 8077 0.000183 60 0.32 46.8 0.164 4.3 11.97 2.1 0.5016 1.7 0.829 0.1731 1.2 2620 37 2588 19 -2 10562-024.1 59 20 0.35 56 10082 0.000000 100 0.00 24.4 0.102 7.3 11.86 2.0 0.4831 1.7 0.841 0.1781 1.1 2541 36 2636 18 +4 10562-025.1 112 66 0.61 170 9190 0.000054 134 0.09 47.6 0.168 4.3 12.07 1.7 0.4959 1.4 0.826 0.1765 1.0 2596 31 2620 16 +1 10562-026.1 200 121 0.62 72 8428 0.000136 35 0.24 82.8 0.180 4.9 11.44 1.6 0.4813 1.4 0.899 0.1724 0.7 2533 30 2581 12 +2 10562-027.1 63 44 0.72 125 9134 0.000110 32 0.19 28.8 0.181 5.3 13.26 2.0 0.5308 1.7 0.834 0.1812 1.1 2745 37 2664 18 -4 10562-028.1 83 41 0.51 84 10623 0.000058 85 0.10 33.0 0.133 5.2 11.09 2.1 0.4608 1.9 0.887 0.1746 1.0 2443 38 2602 16 +7 10562-029.1 85 62 0.75 89 9236 0.000000 100 0.00 35.9 0.218 4.3 12.07 2.1 0.4908 1.9 0.895 0.1783 0.9 2574 40 2637 16 +3 10562-030.1 30 16 0.55 128 8773 0.000286 45 0.50 12.3 0.152 7.7 11.79 3.3 0.4726 2.8 0.855 0.1810 1.7 2495 59 2662 28 +8 10562-032.1 76 82 1.11 79 8279 0.000085 29 0.15 33.6 0.304 3.7 12.92 2.9 0.5140 2.7 0.942 0.1824 1.0 2674 59 2675 16 +0 10562-033.1 159 76 0.49 269 9126 0.000000 100 0.00 74.7 0.137 3.8 14.29 1.6 0.5459 1.5 0.919 0.1898 0.6 2808 34 2741 11 -3 10562-034.1 42 28 0.69 246 9864 0.000153 29 0.27 18.3 0.186 6.1 13.21 2.3 0.5117 1.9 0.824 0.1872 1.3 2664 41 2718 21 +2 10562-035.1 75 61 0.84 142 9390 0.000211 41 0.37 33.0 0.214 4.3 12.83 1.9 0.5110 1.6 0.810 0.1820 1.1 2661 34 2671 19 +0 10562-036.1 122 66 0.56 154 10349 0.000090 36 0.16 47.2 0.167 4.2 9.84 1.6 0.4505 1.4 0.846 0.1585 0.9 2397 28 2439 15 +2 10562-037.1 45 38 0.87 156 9642 -0.000093 50 -0.16 17.9 0.252 5.6 12.14 2.8 0.4672 2.4 0.882 0.1884 1.3 2471 50 2728 21 +11 10562-038.1 301 144 0.49 84 10872 0.000025 144 0.04 122.9 0.143 2.9 11.35 1.5 0.4760 1.3 0.895 0.1729 0.7 2510 27 2586 11 +4 10562-040.1 110 86 0.81 120 10234 0.000065 33 0.11 47.5Draft 0.232 3.7 12.10 1.7 0.5050 1.4 0.857 0.1737 0.9 2635 31 2594 14 -2 10562-041.1 93 39 0.44 237 9380 0.000082 35 0.14 36.6 0.123 5.8 11.26 1.5 0.4581 1.2 0.801 0.1783 0.9 2431 24 2637 15 +9 10562-042.1 71 37 0.54 150 9640 0.000111 29 0.19 30.0 0.168 7.6 12.28 1.9 0.4930 1.6 0.858 0.1806 1.0 2584 35 2659 16 +3 10562-044.1 163 128 0.81 130 9964 0.000067 46 0.12 68.1 0.219 3.3 11.78 1.3 0.4868 1.1 0.851 0.1755 0.7 2557 23 2611 11 +2 10562-048.1 216 117 0.56 328 8992 0.000085 38 0.15 94.6 0.145 3.4 13.07 1.2 0.5090 1.1 0.882 0.1862 0.6 2652 24 2709 10 +3 10562-049.1 71 59 0.85 218 9328 0.000316 26 0.55 31.1 0.235 4.7 13.11 2.0 0.5095 1.6 0.820 0.1866 1.1 2655 35 2712 19 +3 10562-050.1 69 27 0.41 185 9002 0.000424 24 0.74 29.9 0.088 7.2 12.84 1.7 0.5064 1.3 0.723 0.1839 1.2 2641 27 2688 20 +2 10562-051.1 214 76 0.37 246 10766 0.000012 214 0.02 87.8 0.107 4.2 11.47 1.3 0.4769 1.2 0.885 0.1744 0.6 2514 24 2600 10 +4 10562-052.1 83 47 0.59 89 10070 0.000116 37 0.20 34.5 0.186 4.9 11.90 1.5 0.4857 1.2 0.785 0.1777 1.0 2552 25 2632 16 +4 10562-054.1 74 88 1.23 289 8543 0.000141 37 0.24 32.8 0.341 3.8 12.82 1.6 0.5149 1.2 0.776 0.1806 1.0 2677 27 2659 17 -1 10562-056.1 122 94 0.79 116 9357 0.000091 25 0.16 52.2 0.243 3.5 12.07 1.4 0.4961 1.1 0.833 0.1765 0.8 2597 24 2621 13 +1 10562-057.1 79 48 0.63 176 9087 0.000112 53 0.19 34.5 0.172 5.1 12.84 1.6 0.5098 1.2 0.778 0.1827 1.0 2656 27 2677 16 +1 10562-058.1 36 22 0.64 126 9263 0.000161 36 0.28 15.8 0.190 7.3 13.22 2.6 0.5140 2.2 0.845 0.1865 1.4 2674 48 2712 23 +2 10562-059.1 37 23 0.65 152 9014 0.000213 33 0.37 17.4 0.168 7.5 13.92 2.6 0.5439 2.2 0.843 0.1857 1.4 2800 50 2704 23 -4 10562-060.1 117 56 0.50 284 8570 -0.000021 89 -0.04 51.3 0.157 4.4 13.21 1.4 0.5116 1.2 0.843 0.1873 0.7 2663 25 2719 12 +2 10562-063.1 104 42 0.42 127 10134 0.000241 38 0.42 43.4 0.116 5.5 11.71 1.6 0.4882 1.2 0.742 0.1739 1.1 2563 25 2596 18 +2 10562-064.1 171 103 0.62 155 9923 0.000013 214 0.02 71.7 0.168 3.6 11.67 1.3 0.4866 1.1 0.860 0.1739 0.7 2556 23 2596 11 +2 10562-066.1 85 87 1.06 257 8715 0.000230 41 0.40 36.9 0.286 8.8 12.94 1.6 0.5067 1.2 0.747 0.1851 1.1 2643 26 2699 18 +3 10562-067.1 221 89 0.42 207 9792 0.000052 32 0.09 90.3 0.108 4.0 11.29 1.2 0.4750 1.1 0.884 0.1724 0.6 2506 22 2581 10 +4 10562-068.1 78 52 0.69 219 8343 0.000411 22 0.71 33.8 0.176 5.0 12.50 1.7 0.5048 1.2 0.740 0.1796 1.1 2634 27 2650 19 +1 10562-069.1 636 804 1.30 314 5050 0.000005 214 0.01 199.6 0.373 2.0 6.30 1.1 0.3652 1.0 0.921 0.1251 0.4 2007 18 2030 8 +1 10562-070.1 115 46 0.41 199 10919 0.000070 26 0.12 49.9 0.117 5.2 13.26 1.5 0.5058 1.3 0.863 0.1902 0.7 2639 28 2744 12 +5 10562-071.1 243 160 0.68 362 7682 0.000029 31 0.05 117.6 0.185 2.7 16.06 1.2 0.5642 1.1 0.922 0.2065 0.5 2884 26 2878 8 -0 10562-073.1 86 50 0.60 122 9219 0.000000 100 0.00 35.6 0.173 5.1 11.92 1.6 0.4830 1.4 0.838 0.1789 0.9 2541 29 2643 15 +5 10562-074.1 94 46 0.51 170 8363 0.000191 23 0.33 40.1 0.135 5.6 12.05 1.5 0.4967 1.2 0.787 0.1760 0.9 2600 26 2615 16 +1 10562-076.1 74 28 0.39 165 8474 0.000139 29 0.24 33.4 0.114 6.4 13.85 1.6 0.5253 1.2 0.790 0.1912 1.0 2722 27 2753 16 +1 10562-077.1 149 86 0.59 243 8061 0.000055 37 0.10 62.8 0.165 3.6 11.70 1.3 0.4894 1.1 0.863 0.1734 0.6 2568 23 2591 11 +1 10562-078.1 90 68 0.78 90 9545 0.000115 23 0.20 39.4 0.219 4.2 12.25 1.8 0.5086 1.2 0.641 0.1748 1.4 2650 25 2604 23 -2 10562-079.1 113 77 0.71 138 11208 0.000098 53 0.17 48.0 0.190 4.4 12.42 1.5 0.4956 1.2 0.799 0.1818 0.9 2595 25 2669 15 +3 10562-080.1 153 56 0.38 198 9388 0.000192 37 0.33 63.0 0.104 5.0 11.37 1.4 0.4811 1.1 0.786 0.1715 0.9 2532 24 2572 15 +2 10562-081.1 61 20 0.34 168 7847 0.000122 35 0.21 27.7 0.102 7.7 13.92 1.7 0.5257 1.3 0.774 0.1921 1.1 2723 29 2760 17 +2 10562-082.1 112 39 0.36 217 10766 0.000102 104 0.18 47.4 0.098 6.6 11.68 1.7 0.4918 1.2 0.713 0.1722 1.2 2578 26 2579 20 +0 10562-083.1 189 139 0.76 139 10988 0.000123 28 0.21 80.0 0.225 4.4 11.59 1.4 0.4916 1.2 0.863 0.1710 0.7 2578 25 2568 12 -0 10562-084.1 178 105 0.61 311 8269 0.000145 21 0.25 76.4 0.174 3.8 12.53 1.4 0.5005 1.2 0.864 0.1816 0.7 2616 26 2667 12 +2 10562-088.1 458 535 1.21 440 9901 0.000022 30 0.04 157.4 0.346 1.1 7.53 1.2 0.4003 1.1 0.953 0.1365 0.4 2171 21 2183 6 +1 10562-089.1 279 99 0.37 91 11719 0.000313 16 0.54 107.7 0.107 2.3 10.17 1.3 0.4488 1.2 0.894 0.1644 0.6 2390 23 2501 10 +5

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10562-095.1 125 104 0.86 133 9920 0.000618 22 1.07 51.9 0.253 2.2 11.55 2.0 0.4842 1.6 0.762 0.1731 1.3 2545 33 2587 22 +2 10562-119.1 91 100 1.14 292 8509 0.000538 31 0.93 39.4 0.323 3.8 12.77 2.2 0.5057 1.5 0.666 0.1831 1.7 2638 32 2681 27 +2

Wopmay River psammite, W (#11vj9205a) *524209m E, 7182680m N 10812-001.1 379 141 0.38 482 11382 0.000010 70 0.02 114.4 0.114 1.2 5.88 1.3 0.3513 1.3 0.981 0.1214 0.2 1941 21 1977 4 +2 10812-002.1 42 46 1.13 193 9371 0.000083 83 0.14 17.9 0.327 1.8 11.84 1.6 0.4951 1.4 0.885 0.1735 0.7 2593 30 2591 12 -0 10812-004.1 122 52 0.44 244 8782 0.000019 85 0.03 37.3 0.132 1.9 5.98 1.4 0.3563 1.3 0.943 0.1218 0.4 1965 22 1982 8 +1 10812-006.1 120 105 0.91 108 10355 0.000069 45 0.12 50.4 0.252 1.2 11.75 1.3 0.4905 1.3 0.955 0.1738 0.4 2573 27 2594 7 +1 10812-007.1 414 181 0.45 344 11739 0.000038 28 0.07 127.5 0.135 1.1 6.01 1.3 0.3585 1.3 0.978 0.1217 0.3 1975 21 1981 5 +0 10812-008.1 227 105 0.48 191 10938 0.000036 44 0.06 85.2 0.139 1.3 8.82 1.3 0.4368 1.3 0.972 0.1464 0.3 2336 25 2304 5 -2 10812-009.1 50 50 1.04 133 9469 0.000040 10 0.07 21.3 0.300 1.8 11.91 1.4 0.4962 1.3 0.934 0.1741 0.5 2597 28 2597 8 +0 10812-010.1 163 105 0.67 326 7612 0.000018 27 0.03 49.7 0.196 1.3 6.03 1.3 0.3556 1.3 0.963 0.1230 0.4 1961 21 2000 6 +2 10812-011.1 142 48 0.35 139 11505 0.000031 58 0.05 49.4 0.106 1.9 7.72 1.3 0.4057 1.3 0.958 0.1380 0.4 2195 24 2202 7 +0 10812-012.1 310 146 0.49 124 9727 0.000020 46 0.03 91.4 0.144 1.2 5.61 1.3 0.3427 1.3 0.974 0.1187 0.3 1900 21 1937 5 +2 10812-014.1 109 71 0.67 199 9196 0.000068 46 0.12 33.3 0.186 1.8 5.95 1.4 0.3559 1.3 0.913 0.1212 0.6 1963 22 1974 10 +1 10812-015.1 178 42 0.25 159 11210 0.000013 89 0.02 64.3 0.073 1.9 8.57 1.3 0.4214 1.3 0.972 0.1475 0.3 2267 24 2317 5 +3 10812-016.1 209 53 0.26 450 12743 0.000022 64 0.04 74.5 0.075 1.8 8.38 1.3 0.4156 1.3 0.972 0.1463 0.3 2240 24 2303 5 +3 10812-018.1 405 208 0.53 358 12303 0.000013 45 0.02 147.9 0.156 0.9 8.68 1.3 0.4254 1.3 0.950 0.1479 0.4 2285 24 2322 7 +2 10812-019.1 359 273 0.78 331 10901 0.000013 62 0.02 127.0 0.203 0.9 8.41 1.3 0.4121 1.3 0.984 0.1480 0.2 2224 24 2323 4 +5 10812-020.1 250 212 0.87 252 9119 0.000012 131 0.02 103.0 0.252 0.8 11.50 1.3 0.4792 1.3 0.982 0.1741 0.2 2524 27 2598 4 +3 10812-021.1 122 56 0.48 202 9129 0.000070 59 0.12 36.8 0.139 1.9 5.83 1.4 0.3503 1.3 0.901 0.1206 0.6 1936 22 1965 11 +2 10812-023.1 206 101 0.51 260 8833 0.000010 77 0.02 61.7 0.154 1.4 5.88 1.3 0.3486 1.3 0.966 0.1224 0.3 1928 21 1991 6 +4 10812-024.1 294 343 1.21 149 8601 0.000027 30 0.05 91.9 0.358 0.7 6.28 1.3 0.3641 1.3 0.977 0.1251 0.3 2001 22 2030 5 +2 10812-027.1 213 142 0.69 165 10052 0.000194 12 0.34 75.5 0.187 1.1 8.22 1.3 0.4124 1.3 0.965 0.1446 0.3 2226 24 2283 6 +3 10812-028.1 135 88 0.68 299 7650 0.000035 98 0.06 40.3 0.199 1.5 5.85 1.4 0.3475 1.3 0.918 0.1221 0.6 1922 21 1988 10 +4 10812-029.1 239 110 0.48 367 9471 0.000031 43 0.05 71.8 0.142 1.4 5.94 1.3 0.3500 1.3 0.964 0.1231 0.3 1935 21 2002 6 +4 10812-030.1 203 83 0.42 297 10288 0.002209 5 3.83 74.7Draft 0.084 1.8 6.07 2.1 0.4288 1.3 0.611 0.1027 1.7 2300 25 1673 31 -45 10812-031.1 117 55 0.49 258 8950 0.000068 31 0.12 47.4 0.136 1.6 11.18 1.3 0.4729 1.3 0.963 0.1715 0.4 2496 26 2573 6 +4 10812-032.1 54 30 0.57 216 9106 0.000089 32 0.15 23.9 0.157 2.3 13.43 1.5 0.5202 1.4 0.939 0.1872 0.5 2700 30 2718 8 +1 10812-033.1 257 181 0.73 182 8309 0.000041 37 0.07 77.6 0.201 1.1 5.85 1.3 0.3515 1.3 0.966 0.1207 0.3 1942 22 1967 6 +1 10812-034.1 151 72 0.49 332 8759 0.000074 29 0.13 46.2 0.146 1.6 5.96 1.4 0.3552 1.3 0.946 0.1216 0.4 1960 22 1980 8 +1 10812-035.1 221 122 0.57 462 8753 0.000013 95 0.02 67.3 0.173 1.3 5.94 1.3 0.3540 1.3 0.953 0.1217 0.4 1954 21 1981 7 +2 10812-036.1 445 67 0.16 527 13068 0.000011 70 0.02 135.6 0.046 1.9 5.96 1.3 0.3551 1.3 0.980 0.1218 0.3 1959 21 1983 5 +1 10812-037.1 279 225 0.83 401 9792 0.000039 56 0.07 87.9 0.251 1.0 6.15 1.3 0.3669 1.3 0.960 0.1216 0.4 2015 22 1980 7 -2 10812-038.1 89 67 0.78 296 9822 0.000056 97 0.10 25.9 0.224 1.8 5.48 1.5 0.3402 1.3 0.850 0.1169 0.8 1888 21 1909 14 +1 10812-038.1.2 107 79 0.77 286 10359 0.000123 38 0.21 28.2 0.229 2.0 4.94 1.3 0.3075 1.1 0.830 0.1166 0.7 1728 17 1904 13 +11 10812-038.1.3 119 84 0.72 297 10475 -0.000028 34 -0.05 32.6 0.222 1.8 5.15 1.3 0.3174 1.2 0.940 0.1177 0.4 1777 18 1922 8 +9 10812-038.2 129 68 0.55 288 11158 0.000077 60 0.13 30.3 0.161 1.9 4.44 1.5 0.2738 1.3 0.876 0.1177 0.7 1560 18 1922 13 +21 10812-038.2.2 107 61 0.59 279 10208 0.000109 18 0.19 31.4 0.174 1.9 5.48 1.1 0.3415 1.0 0.913 0.1164 0.5 1894 17 1902 8 +0 10812-038.3 140 75 0.55 308 10311 0.002232 5 3.87 40.8 0.179 1.5 5.47 1.9 0.3388 1.3 0.665 0.1171 1.5 1881 21 1913 26 +2 10812-038.3.2 119 66 0.57 261 9784 -0.000015 51 -0.03 33.4 0.172 1.9 5.32 1.1 0.3256 1.1 0.936 0.1185 0.4 1817 17 1933 7 +7 10812-038.4.1 125 76 0.63 304 10510 -0.000017 142 -0.03 35.8 0.185 1.8 5.45 1.1 0.3340 1.0 0.908 0.1183 0.5 1858 17 1930 9 +4 10812-039.1 291 161 0.57 346 8865 0.000024 52 0.04 90.5 0.164 1.1 6.09 1.3 0.3616 1.3 0.972 0.1221 0.3 1990 22 1987 5 -0 10812-040.1 474 174 0.38 195 10285 0.000595 6 1.03 164.2 0.085 1.4 6.54 1.4 0.4035 1.3 0.932 0.1175 0.5 2185 23 1918 9 -16 10812-041.1 384 96 0.26 220 9071 0.000031 28 0.05 114.2 0.077 1.4 5.74 1.3 0.3459 1.3 0.981 0.1203 0.3 1915 21 1961 5 +3 10812-041.2 782 73 0.10 161 10443 0.000008 70 0.01 225.5 0.028 1.7 5.54 1.3 0.3356 1.2 0.990 0.1198 0.2 1865 20 1954 3 +5 10812-042.1 133 59 0.46 220 8038 0.000019 75 0.03 48.7 0.133 1.7 8.75 1.3 0.4272 1.3 0.961 0.1486 0.4 2293 25 2330 6 +2 10812-043.1 131 48 0.38 184 10536 0.000028 50 0.05 42.0 0.116 2.0 6.63 1.3 0.3746 1.3 0.948 0.1284 0.4 2051 22 2076 8 +1 10812-044.1 136 55 0.42 181 9455 0.000010 73 0.02 48.3 0.127 1.7 8.27 1.3 0.4138 1.3 0.966 0.1450 0.3 2232 24 2288 6 +3 10812-045.1 245 130 0.55 264 9775 0.000043 44 0.08 89.1 0.119 1.4 9.62 1.3 0.4239 1.3 0.975 0.1646 0.3 2278 25 2503 5 +11 10812-046.1 751 271 0.37 376 12874 0.000006 61 0.01 229.0 0.110 0.9 5.91 1.3 0.3552 1.2 0.990 0.1207 0.2 1959 21 1966 3 +0 10812-047.1 460 157 0.35 166 11606 0.000028 22 0.05 136.4 0.106 1.1 5.73 1.3 0.3454 1.3 0.985 0.1204 0.2 1913 21 1962 4 +3 10812-048.1 273 87 0.33 576 10212 0.000024 52 0.04 82.8 0.100 1.5 5.96 1.4 0.3537 1.3 0.974 0.1223 0.3 1952 23 1990 6 +2 10812-050.1 203 83 0.42 200 10342 0.000023 34 0.04 72.9 0.120 1.5 8.51 1.3 0.4184 1.3 0.974 0.1476 0.3 2253 24 2318 5 +3 10812-051.1 128 97 0.78 260 9561 0.000051 69 0.09 39.0 0.240 1.5 5.95 1.4 0.3538 1.3 0.912 0.1220 0.6 1953 22 1986 10 +2 10812-053.1 196 153 0.81 232 10383 0.000057 39 0.10 54.4 0.175 1.4 5.67 1.3 0.3226 1.3 0.952 0.1276 0.4 1802 20 2065 7 +15 10812-054.1 522 225 0.45 298 10694 0.000216 8 0.37 152.1 0.123 1.0 5.59 1.3 0.3394 1.3 0.975 0.1195 0.3 1884 20 1949 5 +4 10812-055.1 319 111 0.36 371 9594 0.000009 91 0.02 95.7 0.107 1.3 5.90 1.3 0.3488 1.3 0.979 0.1226 0.3 1929 21 1994 5 +4 10812-057.1 115 60 0.54 252 7652 0.000138 27 0.24 34.2 0.163 1.7 5.76 1.4 0.3449 1.3 0.906 0.1211 0.6 1910 21 1972 11 +4 10812-058.1 283 156 0.57 166 10425 0.000016 72 0.03 82.9 0.170 1.1 5.57 1.3 0.3408 1.3 0.972 0.1185 0.3 1891 21 1933 5 +3 10812-059.1 449 301 0.69 479 10400 0.000008 94 0.01 138.5 0.206 0.8 6.24 1.3 0.3590 1.3 0.984 0.1261 0.2 1977 21 2044 4 +4 10812-061.1 273 191 0.72 289 8566 0.000052 24 0.09 79.4 0.213 1.0 5.59 1.3 0.3393 1.3 0.973 0.1196 0.3 1883 21 1950 5 +4 10812-063.1 321 160 0.51 227 11275 0.000025 55 0.04 98.6 0.156 1.1 6.04 1.3 0.3581 1.3 0.973 0.1223 0.3 1973 21 1991 5 +1

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10812-064.1 120 52 0.45 212 9322 0.000020 103 0.03 33.4 0.129 2.0 5.51 1.4 0.3254 1.3 0.934 0.1227 0.5 1816 20 1996 9 +10 10812-065.1 445 57 0.13 402 12237 0.000072 16 0.13 135.0 0.035 1.9 5.89 1.4 0.3532 1.3 0.982 0.1210 0.3 1950 22 1971 5 +1 10812-066.1 188 105 0.58 267 7606 0.000000 76 0.00 56.5 0.168 1.4 5.86 1.3 0.3496 1.3 0.966 0.1217 0.3 1933 21 1981 6 +3 10812-067.1 494 57 0.12 491 12390 0.000019 46 0.03 146.2 0.034 1.8 5.76 1.3 0.3443 1.3 0.984 0.1213 0.2 1907 21 1976 4 +4 10812-068.1 665 182 0.28 277 13086 0.000014 29 0.02 236.2 0.083 1.0 8.41 1.3 0.4132 1.3 0.986 0.1477 0.2 2229 24 2319 4 +5 10812-069.1 201 71 0.37 152 9535 0.000014 47 0.02 61.0 0.107 1.6 5.97 1.3 0.3533 1.3 0.969 0.1225 0.3 1951 21 1994 6 +2 10812-073.1 492 272 0.57 413 9638 0.000268 7 0.47 147.4 0.164 0.8 5.89 1.3 0.3489 1.3 0.976 0.1224 0.3 1929 22 1992 5 +4 10812-074.1 398 111 0.29 523 11921 0.000016 48 0.03 119.5 0.087 1.3 5.85 1.3 0.3493 1.3 0.981 0.1215 0.2 1931 21 1978 4 +3 10812-075.1 146 73 0.52 159 10968 0.000041 50 0.07 52.4 0.145 1.6 8.51 1.3 0.4188 1.3 0.959 0.1474 0.4 2255 24 2315 6 +3 10812-077.1 165 84 0.52 219 9410 0.000016 38 0.03 49.6 0.153 1.5 5.92 1.3 0.3495 1.3 0.963 0.1228 0.4 1932 21 1997 6 +4 10812-080.1 278 149 0.56 358 10687 0.000007 164 0.01 81.8 0.165 1.1 5.72 1.3 0.3428 1.3 0.972 0.1211 0.3 1900 21 1972 5 +4 10812-083.1 98 59 0.62 195 8959 0.000040 44 0.07 36.3 0.170 1.7 8.74 1.4 0.4300 1.3 0.949 0.1474 0.4 2306 25 2316 7 +1 10812-086.1 281 118 0.44 197 9791 0.000027 34 0.05 83.0 0.130 1.2 5.75 1.3 0.3444 1.3 0.977 0.1210 0.3 1908 21 1971 5 +4 10812-088.1 227 175 0.79 362 9824 -0.000011 60 -0.02 70.0 0.233 1.1 6.04 1.1 0.3581 1.0 0.968 0.1223 0.3 1973 17 1990 5 +1 10812-089.1 108 65 0.62 246 8018 0.000006 54 0.01 33.2 0.183 1.8 5.97 1.1 0.3569 1.0 0.936 0.1214 0.4 1967 18 1976 7 +1 10812-090.1 203 109 0.55 204 11257 0.000008 271 0.01 61.5 0.159 1.3 5.94 1.1 0.3521 1.0 0.948 0.1225 0.3 1944 17 1993 6 +3 10812-094.1 99 68 0.70 453 6702 0.000090 25 0.16 41.7 0.199 1.6 11.60 1.3 0.4884 1.3 0.962 0.1722 0.4 2564 27 2579 6 +1 10812-095.1 170 115 0.70 164 9863 0.000061 35 0.11 50.8 0.206 1.4 5.70 1.1 0.3485 1.0 0.930 0.1186 0.4 1927 17 1936 7 +1 10812-096.1 294 96 0.34 214 10481 0.000027 52 0.05 107.9 0.102 1.3 9.03 1.1 0.4279 1.0 0.978 0.1530 0.2 2296 20 2379 4 +4 10812-097.1 113 79 0.72 134 9847 0.000048 33 0.08 41.6 0.216 1.5 8.73 1.2 0.4276 1.0 0.895 0.1480 0.5 2295 20 2323 9 +1 10812-098.1 314 197 0.65 413 7726 0.000035 37 0.06 95.8 0.192 1.1 5.91 1.1 0.3549 1.0 0.965 0.1208 0.3 1958 17 1968 5 +1 10812-099.1 387 69 0.18 443 12669 0.000262 8 0.45 117.9 0.047 1.8 5.97 1.1 0.3546 1.0 0.953 0.1222 0.3 1956 17 1988 6 +2 10812-101.1 468 89 0.20 502 12668 0.000018 84 0.03 143.5 0.056 2.7 6.00 1.0 0.3569 1.0 0.970 0.1218 0.3 1967 17 1983 4 +1 10812-102.1 426 164 0.40 212 11851 0.000126 12 0.22 125.2 0.116 1.2 5.70 1.1 0.3424 1.0 0.968 0.1208 0.3 1898 17 1968 5 +4 10812-105.1 155 67 0.45 281 9678 0.000034 37 0.06 47.0 0.131 1.6 5.95 1.1 0.3535 1.0 0.953 0.1221 0.3 1951 17 1987 6 +2 10812-106.1 133 87 0.68 372 9792 0.000032 66 0.06 55.1 0.196 1.4 11.43 1.1 0.4822 1.0 0.957 0.1720 0.3 2537 22 2577 5 +2 10812-108.1 306 153 0.52 413 10193 0.000041 27 0.07 93.3 0.151 1.2 5.99 1.0 0.3555 1.0 0.970 0.1221 0.3 1961 17 1988 5 +2 10812-110.1 511 86 0.17 668 11482 0.000011 63 0.02 157.0Draft 0.050 1.4 6.00 1.0 0.3574 1.0 0.984 0.1217 0.2 1970 17 1982 3 +1 10812-111.1 151 61 0.42 289 10150 0.000027 45 0.05 45.9 0.125 1.7 5.92 1.1 0.3535 1.0 0.950 0.1214 0.3 1952 17 1977 6 +1 10812-112.1 392 156 0.41 318 12227 0.000030 31 0.05 117.4 0.123 1.1 5.85 1.0 0.3481 1.0 0.976 0.1219 0.2 1926 17 1984 4 +3 10812-113.1 294 31 0.11 213 12894 0.000018 60 0.03 89.0 0.027 2.7 5.91 1.0 0.3528 1.0 0.970 0.1215 0.3 1948 17 1979 4 +2 10812-114.1 152 87 0.59 158 9916 0.000017 64 0.03 61.2 0.176 1.4 10.66 1.1 0.4694 1.0 0.966 0.1647 0.3 2481 21 2505 5 +1 10812-116.1 243 222 0.95 334 9673 0.000130 26 0.23 71.8 0.263 1.0 5.78 1.1 0.3442 1.0 0.917 0.1218 0.4 1907 17 1983 8 +4 10812-118.1 246 143 0.60 345 9884 0.000070 26 0.12 73.9 0.175 1.2 5.89 1.1 0.3501 1.0 0.953 0.1219 0.3 1935 17 1985 6 +3 10812-119.1 264 132 0.51 347 10698 0.000007 234 0.01 80.8 0.152 1.3 6.02 1.1 0.3563 1.0 0.957 0.1224 0.3 1965 17 1992 5 +2

*UTM Zone 11, NAD 83 Spot name follows the convention x-y.z; where x = sample number, y = grain number and z = spot number. Multiple analyses in an individual spot are labelled as x-y.z.z Uncertainties reported at 1s% and are calculated by numerical propagation of all known sources of error using Squid version 2.22. Errors in ages are 1s absolute in Ma. f206204 refers to mole fraction of total 206Pb that is due to common Pb, calculated using the 204Pb-method; common Pb composition used is the surface blank (4/6: 0.05770; 7/6: 0.89500; 8/6: 2.13840) * refers to radiogenic Pb (corrected for common Pb) Discordance relative to origin = 100 * (1-(206Pb/238U age)/(207Pb/206Pb age)) Calibration standard 6266; U = 910 ppm; Age = 559 Ma; 206Pb/238U = 0.09059 Th/U calibration: F = 0.03900*UO + 0.85600

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