by John A. Percival

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The Superior Province was assembled from continental fragments and intervening tracts of oceanic crust between 2.72 and 2.68 Ga. Continental blocks (Northern Superior, North Caribou, Winnipeg River, Marmion, Minnesota River Valley, Opatica, Goudalie) retain evidence for distinct evolution during the Paleo- and Mesoarchean and little evidence of continental breakup prior to amalgamation. Neoarchean volcano-plutonic rocks of arc affinity dominate oceanic and continent-margin settings, indicating widespread subduction prior to five collisional events between 2.72 and 2.68 Ga. The 3.0 Ga North Caribou superterrane collided with the Northern Superior superterrane between 2.72 and 2.71 Ga on the north and theWinnipeg River terrane to the south, trapping the English River flysch belt between 2.70 and 2.69 Ga. Docking of the juvenile westernWabigoon terrane occurred at a similar time, followed by collision of theAbitibi-Wawa terrane and syntectonic deposition of Quetico turbidites (2.698-2.690 Ga). The northeastern Superior Province east of Hudson and James bays is dominated by 2.78 to 2.69 Ga plutonic rocks emplaced into older crust (3.8-2.83 Ga). Recent discoveries highlight potential for iron-formation-hosted gold and magmatic Ni-PGE mineralization. Common magmatic and tectonic events are recognized in the northeastern and northwestern Superior, although domains and boundaries have not been correlated.

With the exception of Ni, Cr, Cu, PGE, and Ti deposits hosted by mafic-ultramafic intrusions (2.76-2.74 Ga), major mineral deposits of the Superior Province formed during the arc magmatic and collisional stages of orogenesis. Volcanogenic massive sulphide and rare gold deposits occur in 2.735 to 2.70 Ga calc-alkaline sequences, in back-arc or rifted arc settings. Orogenic lode-gold deposits formed along major and minor structures in greenstone belts and associated plutons during regional deformation between 2.71 and 2.68 Ga.Additional gold mineralization, sporadic rare metal pegmatites, and some hydrothermal deposits were formed between 2.68 and 2.60 Ga during widespread late hydrothermal activity. The occurrence of ancient (to 3.8 Ga) crust in the northern Superior Province may signal diamond potential but it remains uncertain whether cool lithosphere survived intense Neoarchean reworking.

The Archean Superior Province represents the mining heartland of Canada, hosting major camps in the Abitibi district of Ontario-Quebec and the Red Lake region of western Ontario. In addition, the Paleoproterozoic Sudbury structure (1.85 Ga), located on the southeastern edge of the Superior Province, is one of the world’s largest nickel producing regions. This report summarizes information on the geology and metallogeny of the Superior Province compiled in recent syntheses of Ontario (Fyon et al., 1992; Williams et al., 1992) and the Superior Province (Card, 1990; Card and Poulsen, 1998; Skulski and Villeneuve, 1999), augmented by recent work in the western (Corkery et al., 2000; Percival et The Archean Superior Province represents the mining heartland of Canada, hosting major camps in the Abitibi district of Ontario-Quebec and the Red Lake region of western Ontario. In addition, the Paleoproterozoic Sudbury structure (1.85 Ga), located on the southeastern edge of the Superior Province, is one of the world’s largest nickel producing regions. This report summarizes information on the geology and metallogeny of the Superior Province compiled in recent syntheses of Ontario (Fyon et al., 1992; Williams et al., 1992) and the Superior Province (Card, 1990; Card and Poulsen, 1998; Skulski and Villeneuve, 1999), augmented by recent work in the western (Corkery et al., 2000; Percival et The Archean Superior Province represents the mining heartland of Canada, hosting major camps in the Abitibi district of Ontario-Quebec and the Red Lake region of western Ontario. In addition, the Paleoproterozoic Sudbury structure (1.85 Ga), located on the southeastern edge of the Superior Province, is one of the world’s largest nickel producing regions. This report summarizes information on the geology and metallogeny of the Superior Province compiled in recent syntheses of Ontario (Fyon et al., 1992; Williams et al., 1992) and the Superior Province (Card, 1990; Card and Poulsen, 1998; Skulski and Villeneuve, 1999), augmented by recent work in the western (Corkery et al., 2000; Percival et al., 2006b) and northeastern Superior Province (Labbé and Lacoste, 2004; Leclair et al., 2004a,b).

Major contributions to understanding the evolution of the Superior Province have come from U-Pb geochronological and geochemical studies over the past 30 years. Geochronology has provided an absolute time framework for the development of greenstone belt strata, the timing and duration of plutonic, structural, and metamorphic events, and serves as the basis for regional correlation. In addition to characterizing rock compositions, geochemical analyses have been used extensively in trace-element discrimination diagrams to infer geodynamic setting. This approach, which has been instrumental in identifying oreforming environments, is based on the rationale that magma generation processes that impart diagnostic trace-element ratios are controlled by pressure, temperature, and partition coefficients, factors that were also valid in the past. Analyses of the Nd-Sm and Lu-Hf isotopic systems have been essential in defining the distribution of ancient continental and juvenile terranes, particularly within complexly deformed areas.

Major contributions to understanding the evolution of the Superior Province have come from U-Pb geochronological and geochemical studies over the past 30 years. Geochronology has provided an absolute time framework for the development of greenstone belt strata, the timing and duration of plutonic, structural, and metamorphic events, and serves as the basis for regional correlation. In addition to characterizing rock compositions, geochemical analyses have been used extensively in trace-element discrimination diagrams to infer geodynamic setting. This approach, which has been instrumental in identifying oreforming environments, is based on the rationale that magma generation processes that impart diagnostic trace-element ratios are controlled by pressure, temperature, and partition coefficients, factors that were also valid in the past. Analyses of the Nd-Sm and Lu-Hf isotopic systems have been essential in defining the distribution of ancient continental and juvenile terranes, particularly within complexly deformed areas.

The Superior Province forms the core of the North American continent (Fig. 1) and is surrounded by provinces of Paleoproterozoic age on the west, north, and east, and Mesoproterozoic age (Grenville Province) on the southeast. Tectonic stability has prevailed since ca. 2.6 Ga in large parts of the Superior Province. Proterozoic and younger activity is limited to rifting of the margins, emplacement of numerous mafic dyke swarms (Buchan and Ernst, 2004), compressional reactivation, and large-scale rotation at ca. 1.9 Ga, and failed rifting at ca. 1.1 Ga. With the exception of the northwestern and northeastern Superior margins that were pervasively deformed and metamorphosed at 1.9 to 1.8 Ga, the craton has escaped ductile deformation.

Current views regard the Superior Province as a collage made up of small continental fragments of Mesoarchean age and Neoarchean oceanic plates with a complex history of aggregation between 2.72 and 2.68 Ga (Percival et al., 2004a, 2006b) and subsequent post-orogenic effects. Early interpretations of the Superior Province as an example of a purely autochthonous, vertical tectonic regime evolved by the early 1990s to accretionary terrane models in which most assemblage contacts were considered suspect rather than depositional. Recent work has succeeded in distinguishing sequences built upon continental basement (e.g. Red Lake greenstone belt, Sanborn-Barrie et al., 2001) from those of probable oceanic affinity (e.g. central Abitibi greenstone belt, Ayer et al., 2002), giving rise to improved models of tectonic evolution. Sedimentary rocks as old 2.48 Ga unconformably overlie Superior Province granites, indicating that most erosion had occurred prior to ca. 2.5 Ga.

The southern Superior Province (to latitude 52°N) is a major source of mineral wealth. Owing to its potential for base metals, gold, and other commodities, the Superior Province continues to attract mineral exploration in both established and frontier regions.

A first-order feature of the Superior Province is its linear subprovinces of distinctive lithological and structural character, accentuated by subparallel boundary faults (e.g. Card and Ciesielski, 1986). Trends are generally east-west in the south, west-northwest in the northwest, and northwest in the northeastern Superior (Fig. 2). Recent work based on isotopic and zircon inheritance studies has provided a means of “seeing through” the latest structural and magmatic events, particularly in regions dominated by granitic rocks, revealing fundamental age domains across the Superior Province. Several domains of Mesoarchean age are recognized in spite of pervasive Neoarchean magmatism, metamorphism, and deformation (Fig. 3). The term “terrane” is used in the sense of a geological domain with a distinct geological history prior to its amalgamation into the Superior Province during 2.72 to 2.68 Ga assembly events. "Superterranes" show evidence for internal amalgamation of terranes prior to the Neoarchean assembly. “Domains” are defined as distinct regions within a terrane or superterrane.

The oldest continental crust (up to 3.7 Ga) occurs in the Northern Superior superterrane (Skulski et al., 2000) and Inukjuak domain of the northeastern Superior province (David et al., 2003). A large region of ca. 3.0 Ga crust, the North Caribou superterrane (Thurston et al., 1991), which may extend into northern Quebec (Stott, 1997), has been interpreted as the continental nucleus to which other terranes were amalgamated during assembly of the Superior Province (cf. Goodwin, 1968; Thurston et al., 1991; Williams et al., 1992; Stott, 1997; Thurston, 2002). Farther south, the Winnipeg River (WR) and Marmion (MT) terranes are relatively small continental fragments dating back to 3.4 and 3.0 Ga, respectively (Beakhouse, 1991; Tomlinson et al., 2004). In the far south, the Minnesota River Valley terrane (MRVT), of unknown extent, contains remnants of crust as old as ca. 3.6 Ga (Goldich et al., 1984; Bickford et al., 2006; Schmitz et al., 2006). In central Quebec, the Opatica subprovince has Mesoarchean heritage, as do large parts of the northeastern Superior Province (Leclair et al., 2004a).

Domains of oceanic ancestry, identified by juvenile isotopic signatures and lack of Mesoarchean zircon inheritance, separate most of the continental fragments. These dominantly greenstone-granite terranes generally have long strike lengths and record geodynamic environments including oceanic floor, plateaux, island arc, and back-arc settings (e.g. Thurston, 1994). Examples include parts of the Oxford-Stull domain in the north, the western Wabigoon in the west, and the Wawa-Abitibi terrane in the southeastern Superior Province. Rocks formed in these environments host some of the largest massive sulphide deposits of the province, particularly in the Abitibi greenstone belt.

Still younger features, the metasedimentary terranes (Breaks, 1991; Williams, 1991; Davis, 2002), separate some of the continental and oceanic domains. Extending across the entire province, these 50 to 100 km wide belts of metagreywacke, migmatite, and derived granite appear to represent thick synorogenic sequences that were deposited, deformed, and metamorphosed during collisional orogeny. Faults, developed in association with several distinct tectonic events, host a variety of orogenic gold deposits across the province.

Early tomographic images of the Superior Province suggested lithosphere thickness of at least 250 km beneath the craton (Grand, 1987), and possibly as much as 350 km (van der Lee and Nolet, 1997). Analysis of shear-wave splitting indicates prominent east-west anisotropy in the lithosphere (Silver and Chan, 1988; Silver, 1996; Kay et al., 1999a,b), which has been attributed to mantle deformation during Archean tectonism. Musacchio et al. (2004) estimated upper mantle velocities in the 8.3 to 8.8 km.s-¹ range for the western Superior Province, consistent with depleted harzburgite compositions, and lithosphere thickness is estimated at 300 km (Kendall et al., 2002). Beneath the western Superior Province, Kendall et al. (2002) distinguished a northern zone of isotropic upper mantle beneath the North Caribou superterrane that contrasts with a southern zone characterized by east-west anisotropy. These domains, which are separated by a subvertical high-velocity zone, extend to about 300 km depth (Sol et al., 2002). To the north beneath Paleoproterozoic crust of the Trans-Hudson Orogen, the lithosphere is thinner and notably more isotropic (Kendall et al., 2002). Domains resembling those defined seismically are also observed in the electrical conductivity structure. Craven et al. (2001) reported an essentially isotropic mantle beneath the North Caribou superterrane, in contrast to pronounced east-west anisotropy in the south. Subsequent analysis has modeled a steeply north-dipping, tabular, resistive zone separating the two domains, which corresponds approximately to the subvertical high-velocity zone. Both the seismic and electrical structures have been attributed to formation of the Superior craton through subduction-accretion processes (Craven et al., 2001; Kendall et al., 2002). Heat flow in the Superior Province averages 42 ± 8 mW.m-² (Cheng et al., 2002; Rolandone et al., 2003) and the reduced heat flow (mantle component) is consistent with a thermal lithosphere at least 240 km thick (Jaupart et al., 1998), supporting the concept of a thick tectosphere.

Direct control on mantle lithosphere composition is generally acquired from xenoliths in kimberlite pipes. However, the known pipes are not ideally situated to provide comprehensive information. Pipes in the Attawapiskat area sample mantle close to the Superior margin, and indicate mainly lherzolitic compositions and a cool geotherm (Scully, 2000). The compositional range is similar to that from Kirkland Lake pipes (Vicker and Schulze, 1994; Schulze, 1996), where geothermobarometry suggests a warmer geotherm corresponding to surface heat flow of about 40 mW.m-2. Taken together, observations of the Superior Province mantle indicate a cool refractory lithosphere typical of Archean cratons (Jordan, 1978). Individual mantle domains correspond to broad geological features (terranes) and anisotropies of seismic velocity and electrical conductivity are east-trending, coplanar to the dominant penetrative crustal structures.

Gravity and aeromagnetic trends generally correspond well with first-order crustal geological features. Metasedimentary belts define gravity and aeromagnetic lows, whereas greenstone belts form local gravity highs. Gravity data have been inverted to estimate crustal thickness, following removal of near-surface effects (e.g. Nitescu et al., 2003). This approach supports seismic observations of crust thinner, by as much as 9 km, beneath the English River terrane. Seismic reflection profiles in both western (White et al., 2003; Calvert et al., 2004) and eastern Superior (Calvert and Ludden, 1999) generally indicate gently north-dipping structures in southern low-grade regions, changing to southward dips in plutonic gneissic terranes farther north. The vergence patterns have been interpreted in terms of a doubly vergent orogen (White et al., 2003) or crustal-scale synclinorium (Hynes and Song, 2006). Reflectors locally extend beyond the Moho, where they have been interpreted as subduction scars (Calvert et al., 1995; White et al., 2003).

Northern Superior Superterrane

The Northern Superior superterrane (NSS) at the northern fringe of the Superior Province is dominated by granitic and gneissic rocks and has been identified based on fragmentary isotopic evidence from Ontario and Manitoba (Skulski et al., 1999). Supracrustal units in the Assean Lake complex of Manitoba include greywacke with detrital zircon ages up to 3.9 Ga, iron formation, and mafic to intermediate volcanic rocks (Böhm et al., 2000, 2003). The ancient rocks have been strongly reworked by granitoid magmatism at 3.2 to 3.1, 2.85 to 2.81, and 2.74 to 2.71 Ga (Fig. 3), representing evolution in a continental magmatic arc setting, followed by amphibolite-facies metamorphism at 2.68 and 2.61 Ga that may have resulted from collisions during tectonic assembly (Skulski et al., 2000; Böhm et al., 2003). The Northern Superior superterrane is bounded to the south by the North Kenyon fault, which juxtaposes it with the Oxford–Stull terrane and hosts local lode gold occurrences. Prominent ductile shear zones in the eastern Northern Superior superterrane may be Neoarchean or Paleoproterozoic in age. Exploration for diamondiferous kimberlite pipes has been promoted by identification of kimberlite indicator minerals in the Ontario- Manitoba border region (Stone, 2005) and general on-strike correlation with the Victor Pipe in the Attawapiskat area to The Northern Superior superterrane (NSS) at the northern fringe of the Superior Province is dominated by granitic and gneissic rocks and has been identified based on fragmentary isotopic evidence from Ontario and Manitoba (Skulski et al., 1999). Supracrustal units in the Assean Lake complex of Manitoba include greywacke with detrital zircon ages up to 3.9 Ga, iron formation, and mafic to intermediate volcanic rocks (Böhm et al., 2000, 2003). The ancient rocks have been strongly reworked by granitoid magmatism at 3.2 to 3.1, 2.85 to 2.81, and 2.74 to 2.71 Ga (Fig. 3), representing evolution in a continental magmatic arc setting, followed by amphibolite-facies metamorphism at 2.68 and 2.61 Ga that may have resulted from collisions during tectonic assembly (Skulski et al., 2000; Böhm et al., 2003). The Northern Superior superterrane is bounded to the south by the North Kenyon fault, which juxtaposes it with the Oxford–Stull terrane and hosts local lode gold occurrences. Prominent ductile shear zones in the eastern Northern Superior superterrane may be Neoarchean or Paleoproterozoic in age. Exploration for diamondiferous kimberlite pipes has been promoted by identification of kimberlite indicator minerals in the Ontario- Manitoba border region (Stone, 2005) and general on-strike correlation with the Victor Pipe in the Attawapiskat area to the east. Correlation is uncertain between the Northern Superior superterrane and units of similar antiquity in the Inukjuak domain of northern Quebec.

Oxford-Stull Domain

The Oxford-Stull Lake domain, as defined by Thurston et al. (1991), contains some of the largest greenstone belts in the northwestern Superior Province, including the Knee Lake-Gods Lake and Stull Lake belts of Manitoba (Corkery and Skulski, 1998; Syme et al., 1999; Corkery et al., 2006). Mainly basaltic rocks of the Hayes River assemblage have been dated locally in the 2.83 Ga range, and volcanic rocks of the Oxford Lake assemblage fall between 2.729 and 2.719 Ga (Fig. 3; Corkery et al., 2000). The occurrence of coarse clastic sediments (Corkery et al., 2000) and alkaline volcanic rocks (Brooks et al., 1982) along some faults suggests that they were active during deposition of the Oxford Lake assemblage (Corkery et al., 1992). Mafic intrusions are common in some belts, such as at Big Trout Lake, and have some Ni -PGE potential. Plutons of tonalite, granodiorite, and granite underlie large parts of the terrane and yield ages between 2.83 and 2.69 Ga. Isotopic data suggest that the Oxford-Stull terrane evolved in an oceanic setting, possibly on the edge of thinned North Caribou crust (Parks et al., 2006), until ca. 2.71 Ga, when it was juxtaposed with the Northern Superior superterrane along the North Kenyon fault. It is bounded by the Stull-Wunnummin and Gods Lake Narrows shear zones in the south, which host numerous lode-gold occurrences.

North Caribou Superterrane

The North Caribou superterrane (Thurston et al., 1991) is the largest domain with Mesoarchean ancestry of the Superior Province. Basement consists of ca. 3.0 Ga juvenile plutonic and minor volcanic belts (Stevenson and Patchett, 1990; Stevenson, 1995; Corfu et al., 1998; Hollings et al., 1999; Henry et al., 2000), upon which were deposited early (2.98-2.85 Ga) rift-related and younger (2.85-2.71 Ga) arc sequences (Thurston and Chivers, 1990). It was severely reworked by continental arc magmatism at 2.75 to 2.70 Ga. The terrane has wide transitional margins in both the north and south.

In the north, the Oxford-Stull, Munro Lake, and Island Lake domains (Thurston et al., 1991) are inferred to have been formed on thinned crust of the North Caribou superterrane based on the presence of <3.0 model Nd ages of 2.9 to 2.71 Ga volcanic and plutonic rocks and the presence of <3.0 Ga detrital zircons in associated sedimentary units (Skulski et al., 2000). In the Ponask Lake area near the Ontario-Manitoba border, detrital zircons from a quartzitekomatiite sequence indicate a depositional age <2.865 Ga, inferred to date breakup at the northern North Caribou margin (Stone et al., 2004). The main phase of plutonism was followed by localized strain and shear-zone-hosted gold mineralization at ca. 2.685 Ga (Lin and Corfu, 2002), particularly in the Little Stull Lake area near the Ontario-Manitoba border (Jiang and Corkery, 1998; Lin and Jiang, 2001; Lin et al., 2006).

The central North Caribou superterrane is intruded by widespread tonalitic, dioritic, granodioritic, and granitic plutons that crystallized between 2.745 and 2.697 Ga at depths ranging from 18 to 10 km (0.6-0.3 GPa) (Corfu and Stone, 1998; Stone, 1998, 2000). Remnants of ca. 3.0 Ga tonalite and supracrustal rocks are sporadically preserved through the younger magmatism (Krogh et al., 1974; Corfu and Ayres, 1991; Henry et al., 1998;Whalen et al., 2003).Within the greenstone belts, thin packages of quartz arenite-carbonate- komatiite have variably been interpreted as platformal cover strata (Thurston and Chivers, 1990; Thurston et al., 1991) and plume-related rift deposits (Hollings and Kerrich, 1999; Percival et al., 2002a, 2006a). Evidence of early (>2.87 Ga) deformation is recorded in the North Caribou greenstone belt (Stott et al., 1989). The iron formationhosted Musselwhite lode-gold deposit may have formed during development of structures associated with 2.87 Ga pluton emplacement, or during ca. 2.7 Ga events (Fyon et al., 1992).Afew examples of porphyry-style Cu-Mo mineralization occur within the central North Caribou superterrane, including the ca. 2.70 Ga Setting Net Lake (Ayres et al., 1982) and Lang Lake occurrences (Findlay andAyres, 1981).

The Uchi domain preserves a ca. 300 m.y. record of tectonostratigraphic evolution (Fig. 3) along the southern margin of the North Caribou superterrane (Stott and Corfu, 1991; Corfu and Stott, 1993b, 1996b; Hollings et al., 2000; Sanborn-Barrie et al., 2001, 2004). This region hosts some of the largest mineral deposits of the western Superior region, including the Red Lake gold camp. Aeromagnetic trends show the complex structural configuration of supracrustal rocks in a chain of greenstone belts separated by large lobes of plutonic material. The stratigraphic record preserved in the Rice Lake, Wallace Lake, Red Lake, Confederation Lake, Meen-Dempster, Pickle Lake, and Fort Hope greenstone belts reflects a history of rifting beginning ca. 2.99 Ga (Pirie, 1982; Corfu and Wallace, 1986; Corfu and Andrews, 1987; Tomlinson et al., 1998; Tomlinson et al., 2001; Percival et al., 2002a; Sasseville, 2002; Bailes et al., 2003; Sanborn-Barrie et al., 2004; Percival et al., 2006a; Sasseville et al., 2006), followed by a protracted period of continental arc magmatism at 2.94 to 2.91, 2.90 to 2.89, 2.85, and 2.75 to 2.72 Ga, punctuated by one or more unconformities (Stott, 1996; Beakhouse et al., 1999; Henry et al., 2000; Hollings et al., 2000; Rogers et al., 2000; Hollings, 2002; Rogers, 2002; Young, 2003; Sanborn-Barrie et al., 2004). The Rice Lake- Black Island belt contains juvenile rocks of probable backarc affinity (Anderson, 2005; Bailes and Percival, 2005; Percival et al., 2006a). Metavolcanic rocks of the Uchi domain host both world-class gold deposits (Fig. 4) (Andrews et al., 1986; Brommecker, 1991; Poulsen et al., 1996; Dubé et al., 2004; Harris et al., 2006) and massive sulphide mineralization (Nunes and Thurston, 1980; Lesher et al., 1986; Rogers, 2002). Several deformation episodes are recognized within the greenstone belts, including pre-2.74, 2.73, 2.72, and 2.70 Ga events that have produced composite, steep, east-trending fabrics (Parker, 2000; Sanborn- Barrie et al., 2001, 2004; Dubé et al., 2003, 2004; Harris et al., 2006; Rogers, 2001;Young et al., 2006).Multiple ages of gold mineralization are indicated, with the main stage associated with D2 deformation structures prior to 2.712 Ga and late-stage gold localization after 2.701 Ga (Corfu and Andrews, 1987; Dubé et al., 2004). Coarse clastic sedimentary rocks generally represent the youngest strata along the southern margin of the North Caribou superterrane (Devaney, 1999a,b). Where dated, these sequences contain detrital zircons as young as 2.703 Ga, and may be facies equivalents of the marine greywacke turbidites of the English River terrane to the south (e.g. Campbell, 1971; Stott, 1996).

Over 450 km of strike length, the east-trending Sydney Lake - Lake St. Joseph (SL-LSJ) fault separates rocks of the North Caribou margin to the north from metasedimentary schists and migmatitic rocks of the English River terrane to the south. The steeply dipping, 1 to 3 km wide, brittle-ductile fault zone is estimated to have accommodated about 30 km of right-lateral transcurrent displacement and 2.5 km of south-side-up movement (Stone, 1981). The Miniss River fault, which is cut and offset by the Sydney Lake - Lake St. Joseph fault, has an age of ca. 2.68 Ga (Bethune et al., 2000, 2006).

English River Terrane

The English River terrane (ERT) is thought to mark the suture between the North Caribou and Winnipeg River terranes (Corfu et al., 1995). Distinguished from adjacent regions by supracrustal rocks of metasedimentary origin, the English River terrane also displays high metamorphic grade, and a prominent east-west structural grain (Breaks, 1991). Based on the turbiditic nature of its chemically immature greywackes, the setting of the English River terrane has traditionally been considered a fore-arc basin (Langford and Morin, 1976) or accretionary prism (Breaks, 1991). Sedimentary facies vary from submarine fan on the northern margin, with associated banded iron formation (e.g., Griffith Mine), to deep-water wackes further south (Meyn and Palonen, 1980). Detrital zircon studies indicate that the sediments were deposited between 2.705 and 2.698 Ga, after arc activity in volcanic belts (Corfu et al., 1995; Davis, 1996a,b, 1998) and close to the time of collisional orogeny, thereby implying an origin as a synorogenic flysch basin. The small Melchett Lake greenstone belt in the central English River terrane comprises a juvenile, ca. 2.723 Ga calc-alkaline volcanic sequence (Corfu and Stott, 1993b, 1996b; Davis et al., 2000), possibly correlative with the Lake St. Joseph assemblage to the north. Metamorphic conditions in the English River terrane range from middle amphibolite facies near the margins, to low-pressure granulite facies (750-850°C at 0.6- 0.7 Mpa) (Perkins and Chipera, 1985; Pan et al., 1999), coinciding with widespread generation of migmatite and diatexite at 2.691 Ga (Corfu et al., 1995). The main tectonothermal event was followed by a second thermal pulse at 2.669 Ga (op. cit. Pan et al., 1999), intrusion of ca. 2.65 Ga pegmatites (Corfu et al., 1995), and growth of hydrothermal minerals (Pan et al., 1999).

The dominant east-west structural grain of the terrane reflects upright to north-vergent F2 folding of an earlier foliation, which is defined in many areas by migmatitic layering (Breaks, 1991; Hrabi and Cruden, 2001, 2006). The early foliation appears to be a composite fabric that includes primary layering and at least one set of early folds and axial planar foliation. It is particularly well expressed in the Lac Seul area (Sanborn-Barrie, 1988), where early, large-scale northtrending, west-vergent folds were delineated (Hynes, 1997).

Gravity (Nitescu et al., 2003), seismic reflection (White et al., 2003), and seismic refraction (Kay et al., 1999a) profiles collectively indicate that the Moho beneath the combined English River – Winnipeg River terrane is elevated by about 8 km over that in adjacent terranes. A late to post-tectonic adjustment of this style could account for metamorphic pressure estimates up to 0.3 GPa higher within the English River terrane, as well as its slow cooling history (Corfu, 1996; Hanes and Archibald, 1999, 2001). The English River – Winnipeg River boundary separates dominantly metasedimentary rocks of the English River terrane from mainly metaplutonic rocks of the Winnipeg River terrane to the south. Between the two terranes lies the metavolcanic Bird River subprovince in eastern Manitoba, with mafic intrusion- hosted Cr, PGE deposits, and its narrow eastward extension, the Separation Lake greenstone belt (Breaks, 1991). These belts consist dominantly of largely juvenile mafic rocks with ages of ca. 2.78 to 2.73 Ga (Timmins et al., 1985). Depositional contacts have been inferred between English River clastic rocks and both volcanic strata of the Separation Lake belt (Hrabi and Cruden, 2006) and gneissic tonalitic basement to the east (Sanborn-Barrie, 1988). The Separation Lake greenstone belt appears to be in tectonic and intrusive contact with granitic rocks of the Winnipeg River terrane to the south (Blackburn and Young, 2000). The boundary zone is a focus for emplacement of ca. 2.646 Ga rare metal pegmatites (Larbi et al., 1999; Breaks et al., 2003; Smith et al., 2004), including the Tanco and Separation Rapids fields (Blackburn and Young, 2000).

Winnipeg River terrane

The Winnipeg River terrane is a collective term used to describe the plutonic domain exposed north and east of the western Wabigoon terrane (Fig. 5). It consists of two main elements: 1) the Winnipeg River subprovince proper (Beakhouse, 1991), a more than 500 km long terrane composed of Mesoarchean metaplutonic rocks variably intruded by Neoarchean plutons; and 2) a largely Neoarchean plutonic domain, formerly referred to as the central Wabigoon granitoid complex (Percival et al., 2002b) and Wabigoon diapiric axis (Edwards and Sutcliffe, 1980; Thurston and Davis, 1985), that contains scattered remnants of Mesoarchean crust (Tomlinson and Percival, 2000; Whalen et al., 2002, 2004b; Tomlinson et al., 2004).With inheritance dating back to ca. 3.4 Ga (Henry et al., 2000; Tomlinson et al., 2003), the Winnipeg River terrane stands apart from the Northern Superior and North Caribou superterranes to the north (Fig. 3) and the Marmion domain to the south (described below). It also carries a distinct record of magmatic and structural events (Percival et al., 2004b; Melnyk et al., 2006), typically characterized by amphibolite- to granulite- facies metamorphism (Corfu, 1988).

The Mesoarchean history of the Winnipeg River terrane has remained cryptic due to extensive overprinting Neoarchean magmatism and deformation. Tonalitic rocks are the oldest units recognized, and include both 3.32 to 3.05 Ga gneissic (Corfu, 1988; Davis et al., 1988; Melnyk et al., 2006) and 3.04 Ga foliated varieties (Krogh et al., 1976). Similar isotopic signatures characterize younger (2.88, 2.84, and 2.83 Ga) tonalitic rocks, reflecting the antiquity of the basement (Beakhouse et al., 1988; Beakhouse and McNutt, 1991). Mafic volcanic belts older than ca. 3.0 Ga (Davis et al., 1988) and ca. 2.93 to 2.88 Ga volcanic rocks in the eastern Savant-Sturgeon greenstone belt (Sanborn-Barrie and Skulski, 1999; Sanborn-Barrie et al., 2002) are also considered part of theWinnipeg River terrane. Significant pulses of Neoarchean tonalite-granodiorite magmatism occurred at 2.715 to 2.705 Ga followed by emplacement of granites at ca. 2.70 to 2.69 Ga (Beakhouse et al., 1988; Corfu, 1988, 1996; Beakhouse, 1991; Cruden et al., 1997, 1998). A complex Neoarchean structural-metamorphic history began with deposition of metasedimentary rocks after 2.72 Ga (Melnyk et al., 2006). The supracrustal rocks and older gneisses were folded (D₃) between 2.717 and 2.713 Ga, prior to syntectonic injection of 2.713 to 2.707 Ga tonalite and granodiorite sheets accompanying D₄ horizontal extensional deformation (Melnyk et al., op. cit.). Upright folding during D₅ deformation took place after 2.705 Ga, and younger upright F6 folds indicate a period of north-south compression associated with emplacement of 2.695 to 2.685 Ga granite and granodiorite (op. cit.). Late pegmatites and granites intruded during a dextral transpressive (D₇) regime (op. cit.).

The eastern Winnipeg River terrane hosts east-trending greenstone belts, including the Caribou Lake, Obonga, Garden Lake, and Heaven Lake belts, that have ages >3075 to 2703 Ma (Davis et al., 1988; Tomlinson et al., 2002, 2003). Dated granitoid units have ages in the range of 3075 to 2680 Ma (Davis et al., 1988; Whalen et al., 2002) and some of the oldest rocks have εNd values of -1 to +1, suggesting derivation from even older crustal sources (Tomlinson et al., 2004). At least five generations of Neoarchean structures (D1-D5) have been recognized in complex tonalitic gneisses (Schwerdtner, 1992; Brown, 2002; Percival et al., 2003). Mineralization includes polymetallic occurrences in the Caribou Lake belt (Sutcliffe, 1988) and fractionated pegmatites along the English River terrane boundary (Breaks et al., 2003).

The Marmion terrane, formerly included as part of the south-centralWabigoon terrane, is now recognized to consist of 3.01 to 2.999 Ga tonalite (Davis and Jackson, 1988; Tomlinson et al., 2004), upon which the Steep Rock, known for its economic iron deposits, Finlayson Lake and Lumby Lake greenstone belts formed between 2.99 and 2.78 Ga (Stone et al., 2002; Tomlinson et al., 2003). Native silver occurs in a volcanic massive sulphide (VMS) environment within the Lumby Lake belt. Iron deposits in the Steep Rock belt have been upgraded through Cretaceous supergene enrichment (Machado, 1987).

A period of continental arc magmatism in the Winnipeg River terrane (2.72-2.70 Ga) (Corfu, 1988, 1996; Whalen et al., 2002; Melnyk et al., 2006) is attributed to north- and eastward subduction of oceanic rocks (Sanborn-Barrie and Skulski, 2006) followed by 2.708 to 2.701 Ga D₁ deformation. Post-2.704 Ga regional deformation (D₂) across the Wabigoon outlasted deposition of syncollisional coarse clastic sedimentary overlap sequences (i.e. Crowduck and Ament Bay assemblages) (Ayer and Davis, 1997; Fralick, 1997; Sanborn-Barrie and Skulski, 2006). Late faults with both strike-slip and dip-slip motion define the present terrane boundary (Gower and Clifford, 1981).

Wabigoon Terrane

TheWabigoon terrane has long been recognized as a composite terrane comprising volcanic-dominated domains with a central axis of variable-age plutonic rocks (Davis and Jackson, 1988; Percival et al., 2002b; Percival and Helmstaedt, 2004). It consists of distinct western and eastern segments.

Western Wabigoon Terrane

The westernWabigoon terrane is dominated by mafic volcanic rocks with large tonalitic plutons (Blackburn et al., 1991). Volcanic rocks range in composition from tholeiitic to calc-alkaline, and are interpreted to represent ocean floor or plateau and arc environments, respectively (Ayer and Davis, 1997; Ayer, 1998b; Ayer and Dostal, 2000; Wyman et al., 2000). Volcanic rocks were deposited between ca. 2.745 and 2.72 Ga (Corfu and Davis, 1992), with the exception of rare older rocks, such as the 2.775 Ga (Davis et al., 1988) Fourbay assemblage of oceanic plateau affinity (Sanborn- Barrie and Skulski, 1999) and minor younger (2.713- 2.70 Ga) volcanic-sedimentary sequences. Plutonic rocks range from broadly synvolcanic batholiths composed of tonalite-diorite-gabbro (ca. 2.735-2.72 Ga) (Davis and Edwards, 1982; Corfu and Davis, 1992; Whalen et al., 2004b), to younger granodiorite batholiths and plutons (ca. 2.710 Ga) (Davis and Edwards, 1986; Sanborn-Barrie, 1988; Davis and Smith, 1991; Melnyk et al., 2006), monzodiorite plutons of sanukitoid affinity (ca. 2.698-2.690 Ga) (Stern and Hanson, 1991; Ayer, 1998a; Stevenson et al., 1999), and plutons and batholiths of monzogranite (2.69-2.66 Ga) (Schwerdtner et al., 1979; Sanborn-Barrie, 1988; Melnyk et al., 2000) (Fig. 3). Immature clastic metasedimentary sequences are preserved in narrow belts within volcanic sequences. They are commonly younger than the volcanic rocks, as illustrated by local unconformable relationships (Fralick, 1997) and geochronological constraints indicating deposition between ca. 2.711 and <2.702 Ga (Davis, 1996a,b, 1998; Fralick and Davis, 1999). Virtually all carry ancient (>3 Ga) detrital zircons indicating old components in source regions. At least two phases of deformation affected supracrustal rocks of the western Wabigoon terrane (Blackburn et al., 1991), with apparent diachroneity in the onset of deformation from ca. 2.709 Ga in the Lake of the Woods area (Davis and Smith, 1991; Ayer and Davis, 1997; Melnyk et al., 2006), to ca. 2.700 Ga in the Sioux Lookout - Savant area in the east (Sanborn-Barrie et al., 1998, 2002; Sanborn-Barrie and Skulski, 2006). These events involved at least local tectonic inversion, through thrust imbrication (Davis et al., 1988) and possible formation of nappe-like structures (Poulsen et al., 1980).

The Sturgeon - Savant greenstone belt, which hosted the Sturgeon Lake massive sulphide camp (Figs. 6, 7; Franklin et al., 1975; Galley et al., 2000), consists of several tectonostratigraphic packages, including the Jutten assemblage of continental rift origin (Sanborn-Barrie et al., 2002), the ca. 2775 Ma Fourbay assemblage, and 2745 to 2735 Ma arc-like sequences, the Handy Lake and South Sturgeon assemblages (Davis et al., 1985; Sanborn-Barrie and Skulski, 1999; Sanborn-Barrie et al., 2002). The 2735 Ma Lewis Lake batholith (Whalen et al., 2004a) may have provided the heat source for seawater convection and massive sulphide mineralization (Galley et al., 2000). Younger (ca. 2718 Ma, Davis et al., 1988), high Fe, Ti basalt and minor dacite of the central Sturgeon assemblage represent a rifted arc sequence. Associated sedimentary rocks contain both arc (2745- 2730 Ma) and continental (3.1-2.8 Ga) detritus (Skulski et al., 1998a). Two younger sedimentary sequences complete the stratigraphic record: 1) greywacke – iron formation (ca. 2.705 Ga) of the Warclub assemblage; and 2) sandstone and arkose (<2.698 Ga) of the synorogenic Ament Bay assemblage (Sanborn-Barrie et al., 2002). Two sets of ductile structures postdate <2.704 Ga rocks: 1) north-trending upright F1 folds; and 2) east-trending upright D2 folds and penetrative foliation. Pre-D1 folds have been inferred locally (Sanborn- Barrie et al., 1998).

Eastern Wabigoon Terrane

The eastern Wabigoon terrane is a composite terrane with greenstone belts and intervening granitoid plutons that show variable Mesoarchean ancestry (Winnipeg River and Marmion) and Neoarchean oceanic affinity (Stott and Davis, 1999; Tomlinson et al., 2000; Stott et al., 2002). In the northwest part of the belt, the 3.0 to 2.92 Ga Toronto and Tashota assemblages may represent a continental margin sequence built on the Winnipeg River terrane based on their Nd isotopic character (Tomlinson et al., 2004). Calc-alkaline rocks of the 2.74 Ga Marshall assemblage have small massive sulphide deposits (Stott et al., 2002). The central part of the belt is dominated by rocks of oceanic affinity, including 2.78 to 2.738 Ga tholeiitic juvenile pillowed basalt and overlying 2.725 to 2.715 Ga calc-alkaline rocks (Stott et al., 2002). Parts of these assemblages contain widespread hydrothermal alteration and host small massive sulphide deposits (Fig. 6; op. cit.). Across the southern part of the eastern Wabigoon terrane, 2.78 to 2.74 Ga calc-alkaline volcanic rocks were possibly built on Marmion-age substrate (Tomlinson et al., 2004). Unconformably overlying clastic rocks (Albert-Gledhill and Conglomerate assemblages) were deposited after ca. 2.71 Ga.At least two deformation events affected the eastern Wabigoon domain: east-striking D₁ structures (<2.706 Ga) and east-striking, dextral transpressive D₂ shear zones (Stott et al., 2002). A 2.694 Ga pluton provides a lower limit on the age of D₂ deformation (Stott and Davis, 1999).

The Quetico - westernWabigoon boundary is well defined as the Seine River - Rainy Lake fault, in an area known for numerous gold showings and small polymetallic vein deposits (Poulsen, 1985). East of Lake Nipigon, the boundary with the eastern Wabigoon is an imbricate zone with an early history of structural telescoping (Devaney and Williams, 1989; Tomlinson et al., 1996) and the significant, structurally hosted Long Lac vein gold deposits (Lafrance et al., 2004). The Wabigoon-Quetico interface is also marked sporadically by <2.692 Ga coarse clastic rocks of the Seine assemblage (Fralick and Davis, 1999) that were deposited in transtensional basins (Blackburn et al., 1991) or delta fan environments (e.g. Fralick et al., 2006).

Quetico Terrane

The Quetico terrane consists dominantly of greywacke, derived migmatite, and granite. No stratigraphic sequence has been established within the steeply dipping, polydeformed and variably metamorphosed sedimentary succession; however, younging directions are dominantly to the north (Percival, 1989). Depositional age constraints indicate slightly older ages for the northern Quetico (2.698-2.696 Ga, Davis et al., 1990) than for the south (<2.692 Ga, Zaleski et al., 1999), consistent with accretionary prism geometry (Percival and Williams, 1989; Valli et al., 2004).

Several plutonic suites cut metasedimentary units, including early 2.696 Ga tonalite (Davis, 1996a). An early (D₁) deformation event predated emplacement of a chain of Alaskan-type mafic-ultramafic intrusions in the northern Quetico, which have some Ni-PGE potential (e.g. Pettigrew, 2004). They are associated with alkaline plutons including nepheline syenite and carbonatite with ages in the range 2.69 to 2.68 Ga (Lassen, 2004) and geochemical affinities with the Archean sanukitoid suite (cf. Stern et al., 1989; Stevenson et al., 1999; Lassen, 2004). Two subsequent deformation events (D₂, D₃) were followed by low-pressure, high-temperature metamorphism that reached upper-amphibolite and local granulite facies at ca. 2.67 to 2.65 Ga (Pan et al., 1994, 1998) in the central region and greenschist facies at the margins (Percival, 1989). Coeval, crust-derived granitic plutons and pegmatites, including ca. 2.67 Ga peraluminous granite and ca. 2.65 Ga biotite granite (e.g. Southwick, 1991) have sporadic rare-element mineralization (Breaks et al., 2003).

Tectonic models for the Quetico terrane have favoured forearc settings (e.g. Langford and Morin, 1976; Percival and Williams, 1989; Williams, 1991; Fralick et al., 2006). Depositional ages of ca. 2.698 to 2.690 Ga overlap those of late arc magmatism in theWabigoon. The dominantly sanukitoid plutons of this age may have been triggered by slab breakoff (cf. Sajona et al., 2000).

The southern Quetico boundary separates metasedimentary rocks from the dominantly volcano-plutonic Wawa- Abitibi terrane to the south. Stratigraphic linkages between terranes are evident in some areas (Zaleski et al., 1999; Fralick et al., 2006), although at ca. 2.685 Ga dextral transpressive shear zones are common (Corfu and Stott, 1996a).

Wawa Terrane

Most workers accept a correlation between theWawa and Abitibi terranes across the transverse Kapuskasing uplift. Within the Wawa terrane, volcanism appears to have begun with the 2.89 to 2.88 Ga Hawk assemblage. The 2.745 Ga Wawa and 2.72 Ga Greenwater and Manitouwadge assemblages indicate an oceanic setting. Volcanogenic massive sulphide deposits in the Wawa terrane have similar ages of 2.72 Ga (Figs. 3, 6; Corfu and Stott, 1986; Williams et al., 1991; Sage et al., 1996a,b). Polat et al. (1999) reported a variety of oceanic magma types from the Schreiber belt, and interpreted the belt as a tectonic mélange (Polat et al., 1998; Polat and Kerrich, 1999, 2001).

Relatively late-stage volcanism at ca. 2.695 Ga (Catfish assemblage) took place during D1 thrusting. Subsequent calc-alkalic to alkalic magmatism (ca. 2.689 Ga, Corfu and Stott, 1996a) and associated coarse clastic sedimentation (<2.689 Ga) was followed by emplacement of sanukitoid plutons (2.685-2.68 Ga) and dextral transpressive D₂ deformation.

Mineralization occurs in two main regions: the Michipicoten- Mishubishu belt in the Wawa area, and the Shebandowan-Schreiber belt to the west. The Michipicoten- Mishubishu belt contains mainly Fe and Au deposits with some Ni and vein Cu deposits. Iron deposits are in oxide-, sulphide- and carbonate- facies iron formations that lie stratigraphically above the 2.74 to 2.735 Ga Wawa assemblage. Gold deposits in this region occur in veins associated with shear zones within plutonic rocks of variable composition and age. The Shebandowan-Schreiber belt hosts important gold, iron, volcanichosted massive sulphide (e.g. Manitouwadge) (Peterson and Zaleski, 1999; Zaleski et al., 1999) and intrusion-hosted Ni deposits. The most significant is the Hemlo gold camp, a large disseminated deposit (Muir, 2003) in a strongly deformed, ca. 2.693 to 2.685 Ga volcano-sedimentary sequence (Davis and Lin, 2003). Gold was deposited during D₂ sinistral wrench deformation between 2.680 and 2.677 Ga (op. cit.), likely from fluids derived from granitoid rocks.

The Great Lakes tectonic zone is the unexposed boundary between the Minnesota River Valley terrane and Wawa terrane, identified from aeromagnetic images (Sims and Day, 1993). It is inferred to dip northward based on the presence of isotopic inheritance in plutons of the Vermilion district of the southern Wawa-Abitibi terrane (Sims et al., 1997).

Kapuskasing Uplift

The Kapuskasing uplift represents a 500 km long faultbounded structure that divides the Superior Province into eastern and western halves (Percival and West, 1994). Amphibolite- to granulite-facies tonalite gneiss, paragneiss, mafic gneiss, and anorthosite (2.765-2.66 Ga) represent midto lower crustal levels of the Abitibi-Wawa and Quetico terranes, exposed through east-directed thrusting and sinistral transcurrent motion during the Paleoproterozoic (Percival and McGrath, 1986; Percival and Peterman, 1994). Krogh (1993) noted the similarity between 2.66 to 2.62 Ga ages of high-grade metamorphism of Kapuskasing rocks and the timing of lode gold deposition in the Abitibi terrane (e.g. Zweng et al., 1993; Davis et al., 1994b), and proposed a genetic linkage. Brittle faults are cut by 1.89 and 1.1 Ga alkalic complexes, which have Nb, REE, and phosphate showings and prospects (Sage, 1991). Recent work suggests that the Kapuskasing structure accommodated a 20° counterclockwise rotation of the western Superior with respect to the east (Halls, 2004; Halls and Davis, 2004).

Abitibi Terrane

The Abitibi terrane hosts some of the richest mineral deposits of the Superior Province, including the giant Kidd Creek massive sulphide deposit (Hannington et al., 1999a) and the large gold camps of Ontario and Quebec (Figs. 2, 4; Robert and Poulsen, 1997; Poulsen et al., 2000). Views of the tectono-stratigraphic evolution of the Abitibi terrane have changed markedly from the allochthonous terrane concept introduced in the early 1990s (cf. Jackson and Fyon, 1991; Desrochers et al., 1993; Jackson et al., 1994), to a more traditional autochthonous stratigraphic framework supported by detailed and geochronological and volcanological studies (e.g. Heather, 1998; Ayer et al., 2002; Mueller and Mortensen, 2002). Stratigraphic complexities are explained in terms of evolution of oceanic geodynamic settings from plateau, to arc and rift environments (e.g. Thurston, 1994; Bédard and Ludden, 1997; Kerrich et al., 1999; Wyman et al., 1999, 2002).

The Abitibi terrane has traditionally been considered as northern, central, and southern regions with overlapping tectono-stratigraphic histories. In the northern Abitibi, volcanic assemblages are mainly 2.735 to 2.72 Ga (Ludden et al., 1986; Chown et al., 1992; Legault et al., 2002) and associated with layered intrusions, although units as old as 2.79 Ga are known (Rheaume et al., 2004). The central zone is dominated by plutonic rocks (Chown et al., 1992). Volcanic rocks of 2.71 to 2.695 Ga and their associated mineral deposits are abundant in the southern Abitibi belt (Fig. 8) (Dimroth et al., 1984; Daigneault et al., 2002; Dubé and Gosselin, 2006), although units as old as 2.75 Ga are present. The southern Abitibi has relatively young sedimentary-volcanic deposits including ca. 2.69 Ga greywackes of the Porcupine Group (Bleeker and Parrish, 1996) and 2.677 to 2.673 Ga conglomeratic and alkaline volcanic rocks of the Timiskaming Group (Davis, 2002).

The Matagami-Chibougamau camp of the northern Abitibi terrane is characterized mainly by Cu-Zn massive sulphide deposits, Cu-Zn vein deposits, and some lode-gold deposits. Volcanic strata hosting the sulphide mineralization range in age from ca. 2.73 to 2.715 Ga. Gold occurs in veins within shear zones and iron formations, or as disseminated mineralization associated with felsic intrusions (Figs. 4, 9; Card and Poulsen, 1998). In the central Abitibi, mineralization is restricted to the Normétal belt, and includes massive sulphides in 2.728 Ga volcanic rocks (Mortensen, 1993), as well as vein gold deposits. To the south, the Timmins-Val d’Or region hosts numerous gold deposits associated with the Porcupine-Destor deformation zone (Fig. 9), major Cu- Zn massive sulphide deposits in the Kidd assemblage (Hannington et al., 1999a; Wyman et al., 1999, 2002), komatiite and intrusion-related Ni deposits (Fig. 10), some pegmatitic deposits, and minor porphyry-type mineralization (Card and Poulsen, 1998; Jébrak and Doucet, 2002). The richly gold-mineralized Cadillac-Larder Lake break, which forms part of the southern boundary of the belt, is considered to represent a south-verging thrust carrying the Abitibi rocks over the Pontiac (Fig. 9) (Dimroth et al., 1984; Feng and Kerrich, 1991, 1992; Calvert et al., 1995; Calvert and Ludden, 1999; Ludden and Hynes, 2000; Poulsen et al., 2000; Davis, 2002). An alternative model views the fault zone as deep crustal material expelled on a fold detachment surface (Benn and Peschler, 2005).

Pontiac Terrane

Metasedimentary schist and paragneiss derived from turbiditic greywacke and minor conglomerate dominate the northern Pontiac terrane. Detrital zircons indicate depositional ages <2.685 Ga (Mortensen and Card, 1993; Davis, 2002), and tonalite, granodiorite, and granite plutons range in age from 2.682 to 2.66 Ga. The southern part of the belt includes the Baby-Belleterre greenstone belt, including volcanic rocks as young as 2.682 Ga (Mortensen and Card, 1993). The Pontiac terrane has been interpreted as a southverging fold-thrust belt that was over-ridden by the southern Abitibi terrane (Benn et al., 1994; Calvert and Ludden, 1999; Davis, 2002).

The Benny-Belleterre mineral belt contains the quartzvein hosted Belleterre gold deposit, as well as synvolcanic Ni-Cu sulphides (with some PGEs) in gabbroic sills and small plugs of dunite-gabbro.

Opatica Subprovince

This predominantly metaplutonic domain bounding the Abitibi terrane to the north consists of units ranging from 2.82 Ga tonalite, through 2.77 to 2.70 tonalite-granodiorite, to 2.68 Ga granite and pegmatite (Benn et al., 1992; Sawyer and Benn, 1993; Davis et al., 1994b). Polyphase deformation includes early, west-verging shear zones (<2.72 Ga), overprinted by 2.69 to 2.68 Ga south-vergent structures (Sawyer and Benn, 1993). The Frotet-Evans-Troilus greenstone belt has showings including Cu-Au veins, volcanogenic massive sulphide, iron formation, and intrusion-hosted Ni-Cu (Gosselin, 1996).

Opinaca Subprovince

Metagreywacke, derived migmatite, and granite characterize the Opinaca subprovince. Polydeformed schists occur at the belt margins, whereas the interior portions are metamorphosed to amphibolite and granulite facies. The northern boundary with the La Grande subprovince is a faulted stratigraphic contact (Goutier et al., 2002). The supracrustal rocks are cut by the 2.67 Ga Broadback River granite (Davis et al., 1994b). Mineralization in the Opinaca subprovince includes rare-metal occurrences within peraluminous granites and associated pegmatites (Goutier et al., 2002).

Ashuanipi Complex

The approximately 300 x 300 kmAshuanipi complex consists of high-grade metamorphic and plutonic rocks (Percival et al., 1992). Early sedimentary and volcanic rocks were intruded by a ca. 2.725 Ga tonalite-diorite suite (Percival et al., 2003), then deformed and metamorphosed to granulite facies and subsequently intruded by orthopyroxene-bearing diatexite (Percival, 1991), granite, granodiorite, and syenite (Leclair et al., 2004a).

Mineralization is restricted to small, high-grade gold showings in iron formation and skarns (Moritz and Chevé, 1992; Lapointe and Chown, 1993; Chevé and Brouillette, 1995). The occurrences are unusual in their setting in a granulite- facies terrane.

La Grande Subprovince

The La Grande subprovince consists of distinct sectors with variable tectonic setting. In the west, Mesoarchean basement (3.33-2.79 Ga) is unconformably overlain by the clastic Apple formation, which hosts uranium-gold occurrences (Roscoe and Donaldson, 1988), and 2.75 to 2.73 Ga volcanic strata (Goutier and Dion, 2004). Older strata are present in the Guyer-LG4 sector, including komatiites and related ca. 2.82 Ga sills, which contain Cu and massive sulphide mineralization. The Venus belt in the northeast contains Ni-Cu-PGE showings (Gosselin and Simard, 2001). Juvenile volcanic rocks (2.75-2.70 Ga) of the Eastmain sector are characterized by porphyry and other magmatic mineralization.

Bienville Subprovince

Plutonic rocks of the Bienville subprovince intrude the northernmargin of the La Grande subprovince andmark a transition to dominantly granitic rocks to the north. The 200 km wide domain is underlain by foliated, gneissic, and massive granodiorite to granite with crystallization ages in the 2.73 to 2.68 Ga range (Skulski et al., 1998b; Percival et al., 2001). Xenocrystic zircons and Nd model ages indicate sources as old as 3.3 Ga.

Northeastern Superior Province (Minto Block)

This remote, far-north region of Quebec was underexplored prior to the early 1990s. Following the work of Percival et al. (1992, 1994, 2001), large parts were mapped for the first time at 1:250,000 (see synthesis in Leclair et al., 2004a). Metallogenic studies were carried out in parallel with regional mapping, and the major mineralization types identified (Labbé and Lacoste, 2004).

Domains of the Minto block were defined on the basis of lithology, and structural and aeromagnetic trends and intensity (Percival et al., 1992, 2001; Stern et al., 1994), and were refined by Leclair et al. (2004a) in light of regional map and isotopic constraints (Fig. 3). The Inukjuak domain in the west (Domain I of Leclair et al., 2004a) hosts the ancient (ca. 3.825 Ga) Nuvvuagittuq supracrustal belt (David et al., 2003) and ca. 3.65 Ga tonalitic gneisses, but is dominated by younger plutonic rocks (2.84-2.69 Ga). To the east, the Tikkerutuk domain (II) consists of pyroxene-bearing plutonic rocks,of 3.02 to 2.71 Ga age, that merge into the Bienville subprovince to the south, which is characterized by 2.71 to 2.69 Ga granite and granodiorite. Farther east, the Lake Minto domain (IV) contains metasedimentary and derived migmatitic rocks, in addition to 2.76 to 2.70 Ga pyroxene-bearing plutonic rocks (Percival and Mortensen, 2002). The Goudalie domain (V) forms a central spine consisting of relatively large volcano-sedimentary belts (2.88- 2.71 Ga) with sparse 3.0 Ga tonalite and abundant pyroxene-bearing plutons (2.73-2.68 Ga). In the east-central Minto, the Utsalik domain (VI) consists of highly magnetic (Pilkington and Percival, 1999), 2.74 to 2.69 Ga pyroxene-bearing plutonic rocks with model ages in the 3.0 Ga range (Leclair et al., 2004a). To the northeast, Douglas Harbour domain (VII) consists of two large charnockitic massifs (2.74-2.73 Ga) within an older (2.88-2.75 Ga) tonalitic complex (Bédard, 2003; Bédard et al., 2003; Leclair et al., 2004a). The Diana complex in the northeast underwent pervasive ductile deformation during the Paleoproterozoic (Madore and Larbi, 2001). Percival and Skulski (2000) attributed the ca. 2.70 Ga deformation and high-grade metamorphism in the western Minto block to collisional processes, whereas Bédard et al. (2003) inferred magmatic and diapiric controls.

The northeastern Superior hosts a variety of mineral showings and small deposits that have been classified into syngenetic and epigenetic types (Labbé and Lacoste, 2004). Syngenetic mineralization, occurring mostly within supracrustal belts, includes Algoma-type iron formation, volcanogenic massive sulphide (Labbé and Lacoste, 2001), magmatic Ni-Cu (Labbé, 2005), mafic intrusion-hosted Fe- Ti-V, and porphyry U-Th and Mo (Labbé and Lacoste, 2004). Supracrustal rocks also host most epigenetic types, including disseminated polymetallic sulphide occurrences (Cu-Zn-Ag-Au, Labbé and Lacoste, 2001), gold in iron formation, vein quartz, and shear zones, sulphide Cu-Ni-Ag-Au in veins, rare earth elements in carbonated rocks, and minor U in veins.

Several first-order characteristics of the Superior Province point to the operation of plate tectonics during its assembly in the Neoarchean. Diagnostic features include 1) the presence of discrete continental and oceanic domains; 2) the existence of juvenile, mantle-derived magmatic rocks, including calc-alkaline basalt and sanukitoid-suite rocks, which suggest mantle metasomatism by fluids or melts in suprasubduction zone environments; 3) a southward-propagating array of five, temporally discrete, orogenic events over the 40 m.y. period between 2.72 and 2.68 Ga, which implies lateral accretion; 4) orogenic belts with length scales >1000 km, comparable to modern plate margin dimensions; 5) calc-alkaline granitoid batholiths with dimensions and compositions comparable to those of modern continental magmatic arcs, such as the South Patagonian batholith; 6) long strike-slip faults, indicating lateral movement (e.g. Sleep, 1992); and 7) gently dipping crustal panels and Moho offsets identified on teleseismic and magnetotelluric images in the Abitibi and Western Superior Lithoprobe transects. Collectively, these observations provide support for the concept that the Superior Province evolved at ca. 2.75 to 2.68 Ga through plate tectonic processes akin to those active today. It is important to note that this framework recognizes autochthonous development of stratigraphic sequences on continental margins or in oceanic regimes (i.e. within individual terranes, cf. Thurston, 2002). Thrust and nappe features have been identified locally through detailed structural and geochronological studies (e.g. Poulsen et al., 1980; Davis et al., 1988; Corfu and Ayres, 1991; Corfu and Stott, 1993a), although in general the structural style differs significantly from that of modern fold-thrust belts.

Steeply dipping foliation and steeply plunging folds are dominant in most domains of the Superior Province. In many regions these fabrics trend east-west or northwest and are the youngest penetrative structures in a polyphase chronology. Their nature has generally been attributed to transpressive strain late in the shortening history (e.g. Williams et al., 1992; Stott, 1997; Berclaz et al., 2004; Parmenter et al., 2006). Where evidence for earlier thrusting has been obtained, the structures responsible for stratigraphic repetition are generally not obvious. Accordingly, this style of deformation could be more common than is currently recognized. For example, early recumbent folds have been noted in the southern Wabigoon (Poulsen et al., 1980) and Quetico (Sawyer, 1983) terranes. Other early (D1) structures appear to have formed in upright orientations. In the Red Lake and Sturgeon Lake belts, F1 folds have steep plunges (Sanborn- Barrie et al., 1998, 2001; Sanborn-Barrie and Skulski, 1999, 2006). Similarly, the D1 shear zone at LakeWinnipeg formed as a steep transcurrent structure (Percival et al., 2006a). The early (ca. 2.73 Ga) north-northwest-trending structures in the Red Lake and Confederation Lake belts are anomalous in light of their belt-scale extent and implication of east-west shortening. Similarly, the first folds in <2.704 Ga sedimentary rocks of the English River terrane are oriented northnorthwest (Hynes, 1997). This recurring pattern could reflect structures defining the margins of early nappes or parautochthonous sheets, overprinted by subsequent folding and shortening (cf. Stott and Corfu, 1991).

Structural style varies widely on a regional scale. In the northwestern Superior, narrow sinuous belts of supracrustal rocks occupy synformal keels between plutonic massifs (Thurston et al., 1991), similar to the pattern of the eastern Minto block, where plutonic diapirs appear to dominate the structure (Bédard, 2003). Metasedimentary terranes have steep, linear features, including plutonic sheets. In the lowgrade Abitibi terrane, the structure is dominated by open, upright folds, whereas structural patterns in the western Wabigoon terrane are controlled by large synvolcanic batholiths.

For the most part, the Superior Province has remained tectonically stable since ca. 2.6 Ga; however, ductile reworking occurred locally at the margins in response to ca. 1.9 to 1.8 Ga collisions. In the northwest, the Superior margin was affected by ca. 1.89 to 1.87 Ga continental arc magmatism and 1.82 to 1.79 Ga penetrative deformation related to collision of the Trans-Hudson Orogen (Percival et al., 2005). The Diana complex in the northeast has a similar ductile overprint (Madore and Larbi, 2001). Evidence of brittle Proterozoic reactivation is present locally in the form of new mineral growth along faults (Kamineni et al., 1992), including gold mineralization in parts of the Porcupine Destor fault (Fig. 9; Berger, 2001).

Mineralization events are plotted with respect to stratigraphic age in Figure 3. It is evident that volcanogenic massive sulphide mineralization (Figs. 3, 6) generally formed between ca. 2.74 and 2.70 Ga, with rare older examples. The oldest (2.93-2.74 Ga) VMS deposits occur in the North Caribou superterrane and are characterized by distinct Ag, Pb-rich metal associations (Fyon et al., 1992; Parker, 1998). Progressively younger deposits formed further south, in the Uchi (e.g. 2.742 Ga South Bay deposit), Wabigoon (e.g. 2.735 Ga Sturgeon Lake deposits, Fig. 7), and Abitibi-Wawa terrane (e.g. 2.716-2.703 Ga Noranda (Figs. 6, 8), Kidd Creek, Horne, Laronde deposits), reflecting the north-tosouth younging of arc magmatism. Examination of the setting of these VMS deposits has generally shown rifted arc or back-arc environments in continental or oceanic settings (e.g. Hannington et al., 1999a), associated with high-temperature magmatism including komatiites (Sproule et al., 2002) and FIII rhyolites (Hart et al., 2004). The link between a plume-arc setting and VMS mineralization appears particularly strong in theAbitibi terrane (Wyman et al., 1999, 2002). Gold-rich massive sulphide deposits such as the Horne and Laronde deposits represent a distinct class of VMS mineralization developed in oceanic settings including the Abitibi terrane (Hannington et al., 1999b; Dubé et al., 2006).

The Neoarchean is well known in Archean terranes globally for its massive sulphide "bonanza", and numerous authors have commented on potential underlying causes. Barley et al. (1998) proposed a Neoarchean global event (cf. Condie, 1998) in which plumes produced enriched oceanic crust that, when recycled in subduction zones, generated metal-rich derivative magmas. Similar circumstances of rifted oceanic arc settings surround the Paleoproterozoic VMS "bonanza" (Franklin et al., 1998). Formation of both the Neoarchean (2.73-2.70 Ga) and Paleoproterozoic (1.88- 1.86 Ga) VMS deposits preceded collisional tectonism by 10 to 20 m.y., and it is plausible that impending collisions forced changes in plate stresses (subduction zone shallowing or roll-back), inducing extension within active arc systems that permitted access of deep-seated, metal-rich magmas.

Magmatic Cu-Ni-PGE deposits (Fig. 10) occur in a variety of settings within the Superior Province (Eckstrand and Hulbert, 2006). Komatiitic deposits of the Abitibi terrane resemble the Kambalda type. The remainder are intrusionhosted, related to relatively young, mantle-derived gabbro (e.g Big Trout Lake, Lac des Iles), alkaline ultramafic (Pettigrew, 2004) and sanukitoid rocks (e.g. Entwine Lake).

At a broad scale, most lode-gold deposits (Fig. 4) are related to faults and shear zones, including terrane-bounding structures, although factors such as host rock type, alteration character, and structural chronology all play important roles (Dubé and Gosselin, 2006). These “orogenic gold” deposits formed late in the tectonic cycle, some in association with movement on major faults and others later, through fluid flow along dilatant zones (Robert and Poulsen, 1997; Poulsen et al., 2000; Dubé et al., 2004; Dubé and Gosselin, 2006). Where dated precisely, gold deposits reflect the general southward younging pattern of orogenies across the western Superior Province. For example, gold showings in the Stull Lake area in the north are associated with ca. 2.72 Ga faults (Lin et al., 2006), deposits in the Red Lake camp are ca. 2.713 Ga (Dubé et al., 2004), and deposits within the Abitibi terrane in the southeast are ca. 2.68 Ga or younger (Jemielita et al., 1990; Wong et al., 1991; Zweng et al., 1993). The timing of mineralization may be polyphase (Dubé et al., 2004), and coincides with late magmatic, metamorphic, and hydrothermal effects observed throughout the Superior Province (e.g. Krogh, 1993; Davis et al., 1994a; Moser et al., 1996; Percival and Skulski, 2000).

Fractionated pegmatites are common within metasedimentary terranes, at their margins, and along faults within volcanic-plutonic terranes. They carry rare-element mineralization at widespread locations across the Superior Province and generally represent the youngest Neoarchean event at ca. 2.66 to 2.64 Ga (Corkery et al., 1992; Smith et al., 2004). Some leucogranite plutons of crustal derivation have similar ages, implying a late, province-wide thermal anomaly that some authors have attributed to a widespread lithospheric delamination event. However, in light of the depleted lithosphere still present beneath the Superior Province (e.g. Kendall et al., 2002), including diamondiferous zones, the delamination hypothesis appears unlikely. Percival and Pysklywec (2004) suggested that the late hydrothermal overprint in the Superior Province is related to inversion of the mantle lithosphere cells, which led to cratonic stability.

Metallogenesis constitutes an integral part of Superior Province tectonic development, as illustrated by recurrent patterns of mineralization and associated events in several terranes. Volcanogenic massive sulphide deposits are generally associated with arc volcanic rocks and young systematically southward from ca. 2.74 Ga (Uchi) through 2.73 Ga (Wabigoon) to 2.72 to 2.71 Ga (Abitibi-Wawa). Gold deposits, formed during collisional orogenesis and subsequent transcurrent faulting, reflect progressive southward docking of terranes, from ca. 2.72 Ga in the northwest to 2.68 Ga in the south. Sanukitoid-suite rocks and their associated Cu-Ni-PGE mineralization generally follow collisional deformation within a few million years, again showing regional variation from 2.71 Ga in the north to 2.68 Ga in the south.

Numerous Proterozoic dykes swarms transect the Superior Province, particularly in the south (Buchan and Ernst, 2004). The Matachewan swarm is volumetrically significant, making up almost 5% of bedrock area in northeastern Ontario. Some Ni-Cu mineralization is present in associated mafic sills within lower Huronian strata (e.g. James et al., 2002). Uranium mineralization in basal Huronian strata was derived from ca. 2.5 Ga erosion of the Superior Province to the north (Long, 2004). Significant mineralization is associated with the Paleoproterozoic Nipissing magmatic event, in form of vein silver deposits in sills of the Cobalt plate (Marshall and Watkinson, 2000). Mineralization related to the Keweenawan event (ca. 1.14-1.10 Ga) includes Cu,Ag in basalts and Ni-PGE showings in Logan sills in the Thunder Bay area (e.g. Hart, 2005). Alkaline intrusions of 1.9 to 1.1 Ga age host Ni-PGE mineralization, and carbonatites of similar age host numerous Nb-REE prospects (Sage, 1991). Apatite mined from the 1.88 Ga Cargill carbonatite complex was upgraded by a Cretaceous weathering event. Several kimberlite clusters have been identified within the Superior Province and include both Proterozoic (1.1 Ga, Sage, 2000) and Mesozoic examples (Heaman and Kjarsgaard, 2000). The 180 Ma Victor Pipe (Armstrong and Chatman, 2001) contains diamonds, as do 551 Ma occurrences in the Otish Mountains region (Moorhead et al., 2002).

Situated on the southern edge of the Superior Province, the 1.85 Ga Sudbury Intrusive Complex represents one of the most richly mineralized bodies of the Canadian Shield. Current thinking regards the gabbro-noritic intrusion to have been generated in response to meteorite impact (Ames, 1999; Rousell et al., 2002, 2003; Therriault et al., 2002). Large Ni-PGE deposits, distributed around the perimeter of the intrusion, are localized primarily in the sublayer at the base of the differentiated sill (Therriault et al., 2002; Naldrett, 2003).

Most of the Superior Province has been mapped at scales of 1:250,000 or better. This regional information dates from the 1960s in parts of northern Ontario and Manitoba, and is very recent in northern Quebec. Mapping in regions with high mineral potential has been updated periodically. Remaining knowledge gaps are primarily the result of cover by Phanerozoic strata, glacial deposits, and water. In northern Ontario, recent interpretations using aeromagnetic data and drill core information have extended Superior Province units beneath the James Bay lowlands (Stott and Berdusco, 2000; Stott and Rayner, 2004). The James Bay and southern Hudson Bay region remains poorly understood as a result of cover and lack of aeromagnetic coverage. Improving our understanding of this area has several purposes:

1. resolving tectonic questions concerning the “big bend” in Superior Province structural trends, from east-west in the west and south, to north-south in the northeast (Fig. 2);
2. assessing the distribution of ancient rocks of the Northern Superior superterrane, with applications for diamond exploration; and
3. tracing northwest-trending, gold-mineralized faults and shear zones between northwestern Ontario and north-central Quebec.

Thanks are due to Beth Hillary for GIS support and to Ingrid Kjarsgaard for editorial persistence. Alain Leclair and Phil Thurston made relevant and helpful comments on an early version of the paper.Wayne Goodfellow is thanked for project coordination and management.

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[Click on an image thumbnail to view a larger image, notice]

 

	Figure 1: Tectonic map of North America, showing location of the Archean Superior Province at the core of the Canadian Shield (after Hoffman, 1989). Unlabelled white areas are knowledge gaps due to lack of exposure and geophysical coverage. Greenland and the Baltic shield are restored to their positions prior to opening of the Atlantic Ocean and Labrador Sea. Dashed lines on the Superior Province outline indicate the extent of Phanerozoic cover. MRVT: Minnesota River Valley terrane.
	Figure 2: Mosaic map of the Superior Province showing major tectonic elements. Data sources: Manitoba (1965); Ontario (1992); Quebec (2002) and (Leclair, 2005). Major mineral districts: 1: Red Lake; 2: Confederation Lake; 3: Sturgeon Lake; 4: Timmins; 5: Kirkland Lake; 6: Cadillac; 7: Noranda; 8: Chibougamau; 9: Casa Berardi; 10: Normétal
	Figure 3: Time-stratigraphic correlation chart showing major tectonic elements of the Superior Province and ages of important mineral deposit types. Age data from Skulski and Villeneuve (1999) and more recent sources (see text for details).
	Figure 4: Gold deposits of the Superior Province (from Au deposit database, this volume). Symbol sizes are proportional to deposit size.
	Figure 5: Distribution of terranes in the Wabigoon - Winnipeg River region, western Superior Province (modified after Tomlinson et al., 2004). Nd isotopic data used to establish terrane antiquity (see sources in Tomlinson et al., 2004) are shown as model ages for felsic rocks and as initial & values for mafic rocks.
	Figure 6: Volcanogenic massive sulphide deposits of the Superior Province (from VMS deposit database, this volume). Commodities include Cu, Zn, and Pb. Symbol sizes are proportional to deposit size.
	Figure 7: Simplified geological map of the Sturgeon Lake camp showing distribution of VMS deposits with respect to the Biedelman Bay subvolcanic intrusion (after Galley, 2003).
	Figure 8: Simplified geological map of a cluster of VMS deposits in the Noranda camp. Fourteen deposits occur in bimodal volcanic rocks underlain by the Flavrian-Powell subvolcanic intrusion (modified after Galley et al., 2006).
	Figure 9: Simplified geological map of the Abitibi greenstone belt showing the distribution of major fault zones and gold deposits. Modified from Dubé and Gosselin (2006) and Poulsen et al. (2000).
	Figure 10: Nickel deposits of the Superior Province (from Ni deposit database, this volume). Deposits represent mainly intrusion-hosted Ni-Cu and Ni-Cu-PGE varieties. Symbol sizes are proportional to deposit size.