Major reference: Canadian Journal of Earth Science Special Issue, Feb/March 2000 - The Lithoprobe Abitibi - Grenville transect

    Synopsis
    Within North America the Grenville Province extends from the Labrador coast of Canada to as far to the southwest as Mexico, and perhaps into Australia and Antarctica.
    The global extent of the Grenville orogen - rodkarl2b.jpg

    Grenvillian rocks are subdivided into a set of allochthonous terranes arranged in the form of a southeasterly dipping  thrust stack emplaced over the southern margin of the Archean age Superior Province. Rock units within the thrust stack range in age from Archean to late Mesoproterozoic, with older units occupying the lower levels of the thrust stack, and the younger units the higher levels to the southeast. The first-order subdivision of the Grenville involves recognition of:
       1) an external 'Parautochthonous' belt composed of Archean, Paleoproterozoic, and Mesoproterozic rocks representing the southern margin of Laurentia during the Mesoproterozoic;
       2) an 'Allochthonous polycyclic' belt composed of transported Paleoproterozoic and Mesoproterozoic rocks rocks separated from the 'Parautochthonous belt by the 'Allochthon Boundary Thrust' or 'ABT';
and 3) an 'Allochthonous monocyclic' belt formed of rocks largely of  Mesoproterozoic age.
   Tripartite tectonic subdivision of the Grenville, after Rivers et al., 2000 - grencarr4.jpg

    Each belt is further subdivided into lithotectonic zones on the basis of  the tectono-magmatic history of the rocks present in the zone.
   General map of the southwestern Grenville Province, Carr et al., 2000 - grencarrmap1800.jpg (large image 1800 pixels)
   Allochthonous terranes (2000) of the Grenville Province, Ludden & Hynes, 2000  -grenbelts2.jpg
   The Grenville Province thrust stack, Ludden & Hynes, 2000 - grenxsect.jpg
    Cross section and summary table for Grenville events affecting southwestern Ontario, Carr et al., 2000 - grencarr21800.jpg

    Map showing relative stacking order of the Central Gneiss belt allochthons of the southwestern Grenville, Ketchum & Davidson, 2000 - grenketch2.jpg
    Lithotectonic divisions of the southwest Grenville according to Carr et al., 2000 - grencarr3.jpg
   Map of the Frontenac and Morin zones of Quebec, Corriveau et al., 2000 - grencorrivmap.jpg

    Other than the youngest intrusive granites, all rocks within the Grenville Province were highly deformed and metamorphosed between 1.2 and approximately 1 billion years, and common rock types include quartzofeldspathic gneiss, commonly garnet-bearing,  marble and calc-silicate, quartzite, pelite, meta-volcanic rocks, breccias, metadiabase, anorthosite, gabbro, amphibolite, granulite, eclogite, tonalite, granite, syenite, and migmatite. The least metamorphosed supracrustal rocks are found in the Elzevier terrane, the supposed composite arc allochthon.
    Lithologic-terrane map of the southwestern end of the Grenville Province, anon - grenontadir.jpg
    Rocks formed during Geon 14 (1.5-1.4 Ga), Rivers & Corrigan, 2000 - grengeon14.jpg
    Rocks formed during Geon 13 (1.4-1.3 Ga), Rivers & Corrigan, 2000 - grengeon13.jpg
    Rocks formed during Geon 12 (1.3-1.2 Ga), Rivers & Corrigan, 2000 - grengeon12.jpg

        EpsilonNd data for the Grenville Province
    Nd isotope terranes of the western Grenville Province, Dickin, 2000 - grendickin1.jpg
    Histogram of Epsilon Nd values, western Grenville Province, Dickin, 2000 - grendickin4.jpg
    Nd isotope terranes of the central Grenville Province, Dickin, 2000 - grendickin2.jpg
    Histogram of Epsilon Nd values, western Grenville Province, Dickin, 2000 - grendickin5.jpg
    Nd isotope terranes of eastern Grenville Province, Dickin, 2000 - grendickin3.jpg
    Histogram of Epsilon Nd values, western Grenville Province, Dickin, 2000 - grendickin6.jpg
    Histograms of Epsilon Nd values typical of Grenville terranes, Dickin, 2000 - grendickincomp.jpg
    Tdm model age domains of the Ontario segment of the Grenville Province, Dickin & McNutt, 1990 - grentmnd.jpg

        The Thrust Stack
         It has been argued on the basis of lead isotope data (DeWolf and Mezger, 1994)  that in Ontario Archean crust, or Lower Proterozoic rock derived from the Archean, underlies the northern Grenville Province at least as far to the south  as Parry Sound.
   The Grenville Province thrust stack, Ludden & Hynes, 2000 - grenxsect.jpg
   Lithotectonic zones (2000) of the Grenville Province, Ludden & Hynes, 2000  -grenbelts2.jpg
   General map of the southwestern Grenville Province, Carr et al., 2000 - grencarrmap1800.jpg
   Isotopic data  for the Grenville, Ketchum & Davidson, 2000 - grenketch1.jpg

         The thrust stack, from bottom to top, includes the following rock units:
         1) a parautochthonous unit composed of orthogneiss, quartzofeldspathic and quartzose paragneiss, kyanite-garnet schists, and amphibolites, intruded by the 2.45 Ga River Valley anorthosite-gabbro suite, 1.75 Ga gabbros, 1.75 - 1.605 Ga granitoids, 1.47-1.38 Ga granitoids, 1.268 -1.222 Ga anorthosite (St. Charles, Mercer), 1.244 Ga granitoid bodies, and 1.238 Ga Sudbury diabase.  The gneissses are Archean in age whereas the metasediments and amphibolites may be Paleoproterozoic. Locally, orthoquartzitic metasediments (e.g. the Alban  orthoquartzites) overlie quartzofeldspathic gneisses. The quartzites contain detrital zircons of both Archean (2.7 Ga) and Penokean  (1.885 Ga) age, and have Sm/Nd isotopic characteristics intermediate between  those of Archean rocks to the north and some younger component. The quartzites may have been deposited in a Mesoproterozoic age sedimentary basin located between  the Southern Province and a southerly Penokean or younger arc. Similar quartzites are found along the Ontario - Quebec border northeast of North Bay (D168). The younger source must have been older than 1.47 Ga since the sediments are intruded by granites  of this age.
        The southern part of the parautochthon is occupied by Paleoproterozoic metasedimentary gneisses (Barilia) with ca. 1.9 Ga Nd/Nd model ages. The are thought to  represent a juvenile off-shore 1.86 Ga Penokean arc, possibly an eastern lateral equivalent of the Penokean arc in Wisconsin to the west of the Great Lakes.  As in the case of the rocks further north, the gneisses are intruded by 1.75 and 1.45 Ga granitoids.  Grenvillian granites with ages of 1.25 Ga are well developed in the region of Lake Nipissing. The youngest rocks in the parautochthon are garnet granulite and amphibolite dike segments and boudins representing the remains of Sudbury diabase dikes. They are found in all units as far south as the boundary of the parautochthon with the lowermost unit of the overlying allochthonous thrust stack.
    Distribution of Early Proterozoic structural provinces of the southern and southwestern United States - lprotmazat1.jpg

       2) The lowermost unit of the allochthonous thrust stack, the Algonquin terrane, is composed of high P-T gneisses (containing eclogites and garnet granulites) which exhibit younger much less consistent Nd model ages (1.87-1.56 Ga). Two groups of orthgneiss have been identified, one group with ages ranging from 1.715-1.610 Ga, an age range equivalent to the Yavapai/Mojavie accretion event and the Mazatzal orogeny of the central and southeastern USA, and the other with ages 1.47-1.375 Ga. Some eclogite bodies also have protolith ages of about 1.47 - 1.4 Ga, and metamorphic ages (secondary zircon growth) of 1.09 The Algonquin terrane is also distinguished by the presence of bodies of coronitic olivine metagabbro with protolith ages of 1.16 Ga.
        3) The thrust slice above the Algonquin terrane includes the Shawanaga domain outcropping north of the Parry Sound thrust slice, and the Ahmic, upper Go Home and upper Rosseau windows south of the Parry Sound slice. Protolith ages of granitoids are entirely Mesoproterozoic (1.465-1.300 Ga), and Nd model ages are 1.64-1.46 Ga. Eclogites record the oldest metamorphic ages (1.12 Ga) but peak metamorphism could be as young as 1.08 Ga. If the Algonquin and Shawanaga slices are separate terranes, they were stitched by the 1.16 Ga metagabbro suite.
              Lithologic geologic map and shear zones of Britt domain of the Pointe au Baril - Parry Sound region, Culshaw et al, 1994 - grenshawan.jpg

        4) The Parry Sound thrust slice is composed of highly deformed and metamorphosed mafic meta- igneous rocks bordered to the north by anorthosite, anorthositic gabbro, and amphibolite with an age of c. 1.4 Ga. The slice is thought to be exotic and far travelled from an oceanic domain to the southeast.
        5) The Muskoka slice is composed of 1.455 -1.395 Ga rocks with Nd model ages of 1.62-1.41 Ga. Metamorphism took place at 1.095-1.025 Ga but may also predate 1.1 Ga. The 1.16 Ga metagabbros are represented in the Muskoka slice but eclogite bodies either do not exist or have been converted to amphibolite.
            Those granitic rocks with an age of c. 1.45 Ga are common throughout the  Grenville as far north as the Southern Province-Grenville boundary zone, and are  considered by some to represent a post-orogenic suite of intrusions formed by the melting of older  crust.

        Rocks of the 'Allochthonous monocyclic thrust belt includes three slices: the Central Metasedimentary belt, the Frontenac belt, and the Adirondack-Morin belt.
        6) Grenville supergroup carbonates (marbles) and volcanic rocks (amphibolites)  of the Central Metasedimentary belt. Anorthosite and associated rocks (Morin) intrusive  into this terrain have relatively young Grenville ages (c. 1.0 Ga). The volcanic rocks  appear to be derived from the mantle and either represent a Neoproterozoic rift or  arc marginal basin thrust from the southeast.
            Within the eastern Quebec section of the Grenville Province rocks with model ages of c. 1.5 Ga constitute an oceanic arc terrane referred to as 'Quebecia' by Dickin (2000).  Within Quebecia the 1.41-1.39 Ga La Bostonnais igneous complex represents a younger ensialic arc formed after amalgamation of Quebecia with more internal arc terranes.
        7) Frontenac supergroup carbonates and quartzites with detrital zircons as  young as 1.3 Ga and as old as 1.415, 1.6-1.795, 1.745-2.065, 2.12-2.58, 3.185. The  Frontenac sediments must therefore be younger than 1.3 Ga. They are intruded by 1.17  Ga granites with 1.34 - 1.48 Ga model ages, and quartzofeldspathic gneisses have 1.56 -  2.045 Ga model ages, implying the existence beneath the Frontenac of source material  (either basement or derived sediment) older than 2.05 and younger than 1.34.
       Lithologic domains and shear zones of the Grenville Province of Ontario, Hildebrand & Easton, 1995  - grenhild1.jpg
        Geologic map of the Grenville Frontenac terrane of Ontario, Hildebrand & Easton, 1995 - grenhild2.jpg

        8) The Adirondack-Morin belt is composed of 1.35 Ga gneisses, 1.17 and 1.08 plutonic suites, and 1.15 anorthosite bodies.

 Assembly of the Grenville as a collision zone may have taken place in several stages. Initially with the obduction of the Elzevir and related terranes at 1190-1180 Ma, followed by thrusting of the Frontenac over the Elzevir, and of the Parry Sound terrane over the Central Gneiss belt, at 1161 Ma, and finally with the emplacment of all southerly terranes over the Britt terrane at 1080 - 1050.

         Plate Tectonic models
         Plate tectonic model according to Wasteneys et al., 1999 - grenptectwast.jpg
         Plate tectonic model according to Carr et al., 2000 - grenptectcarr.jpg
         Plate tectonic model according to Corriveau et al., 2000 -grencorriv2.jpg

                                                     Event Sequence for the Grenville Province of Ontario

NW              Britt                   Parry Sound             CMB              SE
1               2                       3                       4                5
                982 ti
                992 m
                995 z melt pods
                1007 late peg
                synkinematic pegmatite z 1019+4
                1030 z Algonquin granite

                                         1047 anatectic granite
                Coronitic metagabbro z   1047+5
                Vertical ductile strain c. 1050 ductile strain
                                        and met retro           Granites 1060
                                        Moon diabase 1062
                Metamorphism 1080       Ahmic diabase 1080      Granites 1080
                and anatexis            1114 dike post-
                                        granul. mig
Keweenawan 1120
                Pegmatite 1150
                                        Dike > 1151                              Morin Anorth. 1159
                                        Shear zone 1159+4
                                        Pegmatite 1160          Kingston diabase 1160
                                        New zircon 1161          <-------        Thrusting 1161
                                        in granulite                             Plutonism 1162
                                        Parry S anorth 1163
                Coronitic metag. b. 1170
        `                                                                        Plutonism 1179
                                                                Obduction of Elzevir 1190-1180
                Mercer Anorth. 1222                             Lavant gabbro 1225
                Sudbury diabase 1238
                                                                                 Charnokite 1250
                St Charles Anorth. 1268
                                        Tonalite gneiss 1314                     Volcanism 1286
                Nobel Gneiss 1330
                                        Parry Sound marginal orthogneiss 1346+69
                                        Whitestone Anorth 1350
                Granitoid 1394
                Orthogneiss 1457

   Lithotectonic map and cross section of the Grenville Gagnon and Molson Lake terranes, southwestern Labrador, Rivers et al., 1993 - grenriv1.jpg
    Diagram illustrating the development of the Grenville foreland fold-thrust belt, Rivers et al, 1993 - grenriv2.jpg
    Geological map of the 'Grenville Front' in the Brodil Lake region, SW of Sudbury, Ontario, after Henderson, 1967 - grenbrodil83.jpg

    The Huronian was tightly folded into a set of east-west trending doubly plunging folds prior to the injection of sheets and dikes of Nipissing diabase at 2.2 Ga. It was then brecciated and injected by fluidized breccia material as a result of the 'Sudbury event' before being subject to two further phases of deformation, the first of which involved penetrative pure shear and the second non-penetrative simple shear.

    On the basis of the common presence of shatter cones in Huronian quartzites south of Sudbury and the distribution of the enigmatic 'Sudbury breccia' and Onaping 'fall-back' rocks, it is thought that the Sudbury basin represents the remains of a Paleoproterozic meteorite impact intruded by a 'circular' body of mafic to felsic material, the Sudbury Irruptive, generated by impact partial melting of Archean and Huronian rocks. The fall-back rocks are overlain by a folded and cleaved succession of mudstones and turbidites, the Whitewater Group. The irruptive is 1.85 Ga old and is deformed and metamorphosed along its southern rim. It is cut by quartz-diabase or 'trap' dykes that are deformed and metamorphosed to amphibolite. Pleochroic amphibole mantles relict cores of pyroxene and amphibole. The 'trap' dikes have chilled margins 'suggesting intrusion into cool Sudbury Irruptive complex rocks'. In contrast, diabase of the Sudbury swarm crossing the Sudbury basin are unmetamorphosed and undeformed.

    At about 1.75 Ga, granitoid bodies (Killarney granites) were intruded after the second deformation event and either prior to or during the third deformation event in both the Cutler and ‘Grenville Front’ areas. The curvature of the Huronian stratigraphy and east-west structural trends (MacGregor Bay fold structure) into parallelism with the the north-east trending ‘Grenville Front’ may be related to this event, since Huronian pelitic rocks are folded by north-west trending folds at the front prior to their conversion to andalusite-cordierite-bearing schists by the granites. To the northeast the relative distribution of Huronian rocks within the granites suggests that a synclinal axis runs through the granites such that to the south-east of the granites the Huronian sucession would face north-west. The folded gneisses to the south-east of the granite belt does include belts of kyanite-garnet-biotite schist perhaps representing metamorphosed Huronian aluminous metasediment (McKim formation) intercalated with Archean basement gneisses. Some quartzite units within this belt are almost certainly Huronian equivalents because they contain detrital zircons of Archean age as well as zircon needles, evidently of metamorphic origin, with an age of 1.7 Ga. Metagabbro bodies injected into these rocks may belong to the Nipissing diabase suite. The gneisses also contain deformed anorthosite-gabbro bodies of early Proterozoic age, and a gabbro-granophyre body dated at 1.75 Ga. The Killarney granites were subsequently injected by the younger 1.4 Ga Bell Lake granite, which was itself non-pentratively deformed along its southern margin prior to injection of the Sudbury diabase suite of dikes.
        Grenville Front in Brodil Township SW of Sudbury, after Henderson, 1967 - grenbrodil83.jpg

    Where the 1.238 Ga olivine-bearing diabases (often containing large xenocrysts of plagioclase) of the Sudbury swarm cut Huronian rocks of the Southern Province, the diabases are straight and only locally faulted. However, when traced into the Grenville Province, the diabase rocks become irregular in form, are cut by non-penetrative ‘brittle’ mylonite zones, and contain metamorphic spinel (cloudy plagioclase) and garnet. Further into the Grenville Province the diabases undergo penetrative ductile deformation and form isolated boudins of pyroxene-garnet or garnet-amphibole rock. Within shear pods the igneous texture of the diabases are easily recognisable in spite of the replacement of plagioclase by garnet. The penetrative deformation recognisable in the diabases represents the Grenville orogeny.
    Distribution of diabase,  metadiabase, metagabbro, cpx-garnet,  and eclogite bodies in the Grenville of Ontario, Ketchum & Davidson, 2000 - grendiabase.jpg
 

   The geological history or the Southern and northern Grenville Provinces therefore likely involved the following events:

1) Deposition of the Huronian sediments and volcanics (and related igneous complexes)

2) Major folding of the Huronian F1

3) Injection of Nipissing diabase sheets and dikes (2.22 Ga)

4) The Sudbury impact event

5) Deposition of the Whitewater sediments

6) Penetrative pure shear deformation of the Huronian and Whitewater rocks F2

7) Intrusion of the Sudbury Irruptive (1.85 Ga)

8) Intrusion of the Sudbury Basin 'trap' diabases

9) Intrusion of the Cutler and Killarney granites (1.75 Ga)

10) Deformation of the Huronian, Sudbury Irruptive (South Range shear Zone),

and Cutler granite F3

11) Late post-granite deformation and metamorphism

12) Intrusion of the Bell Lake Granite (1.47 Ga)

13) Non-pentrative deformation of the Grenville Front rocks (? Ga)

14) Injection of the Sudbury Diabase dike swarm (1.238 Ga)

15) Grenville deformation and metamorphism (ca. 1.0 Ga) F4

16) Injection of the Grenville dike swarm (575 Ma)

Lambert-David-D; Frick-Louise-R; Foster-Jeffrey-G; Li-Chusi; Naldrett-Anthony-J., 2000. Re-Os isotope systematics of the Voisey's Bay Ni-Cu-Co magmatic sulfide system, Labrador, Canada; II, Implications for parental magma chemistry, ore genesis, and metal redistribution. In: A special issue on Voisey's Bay Ni-Cu-Co deposit.  Naldrett-Anthony-J (editor); Li-Chusi (editor),  Economic Geology and the Bulletin of the Society of Economic Geologists. 95; 4, p  867-888.
   AB: Re-Os isotope data have been obtained for sulfide samples from five environments within the 1333 Ma Voisey's Bay intrusion (Ovoid, Eastern Deeps, Discovery Hill zone, Reid Brook zone, and Basal Breccia sequence) and the 1313 Ma Mushuau intrusion (Sarah prospect), as well as unmineralized gabbroic and troctolitic intrusions, Archean Nain orthogneiss, and Proterozoic Tasiuyak paragneiss, in order to assess the role of crustal contamination in the genesis of this large Cu-Ni-Co sulfide deposit.
        Massive sulfide samples have high Re concentrations (148-288 ppb) compared to their Os concentrations (4.8-28 ppb), yielding high Re/Os ratios (2.9-38) that are similar to those for massive sulfides from Sudbury and the Duluth Complex. Whole-rock Re-Os isotope data exhibit a large spread in 187Re/188 Os (14-157) but do not define a precise isochron, most likely the result of R factor variations within this dynamic ore system (R factor = effective mass of silicate magma with which a given mass of sulfide magma has equilibrated). Large whole-rock sulfide samples from the Ovoid yield an imprecise 1320 Ma isochron age that is consistent with baddeleyite U-Pb ages from the magmatic system. However, data for sulfide (chalcopyrite, pyrrhotite, pentlandite) and oxide (magnetite, ilmenite) mineral separates from the Ovoid and a troctolite from the Eastern Deeps yield and isochron with an age of 1004+/-20 Ma, consistent with Re-Os TCHUR model ages for some low Os troctolites and olivine gabbros from the magmatic system. These data suggest that the Re-Os system may have been reset at the mineral scale and metals redistributed during a heating-hydrothermal alteration event which coincided temporally with the Grenville orogeny. The high initial gammaOs values (200-1,100 = percent deviation in calculated initial 187Os/ 188Os from mantle of the same age) for sulfide-rich samples from the Voisey's Bay intrusion document significant magma interactions with older Nain-Churchill province crust as there are no known mantle reservoirs with these extreme geochemical characteristics. Re-Os isotope modeling suggests that a reasonable fit to the sulfide data may be obtained via contamination of basaltic magma similar to fine-grained feeder zone olivine gabbros and troctolites with sulfidic-graphitic Proterozoic Tasiuyak paragneiss (gammaOs = 1,900), followed by an R factor process (300->5,000) that improved the tenor (metal concentration in 100% sulfide) of the sulfide liquid during transport in the active Voisey's Bay magma conduit or after deposition in the active-replenished Eastern Deeps magma chamber. However, R factors of this magnitude (>5,000) are not supported by Cu, Ni, and PGE data for the mineralization. Thus, chalcophile element-depleted feeder olivine gabbros and troctolites from the Voisey's Bay intrusion may represent frozen magmas that were the end product of sulfide saturation and segregation during the early stages of mineralization. More internally consistent R factors (50-500) are obtained if the immiscible sulfide magma interacted with a second, chalcophile element-undepleted (>150 ppt Os) magma.
        Compelling evidence for the presence of more fertile magmas in the Voisey's Bay system comes from the geochemical and Re-Os isotope data for unmineralized melatroctolite inclusions within the Basal Breccia sequence. These inclusions contain olivine with high MgO and Ni concentrations and low La/Sm and Th/Nb ratios, a high Os concentration, and an enriched (but near-chondritic) initial Os isotope composition (gammaOs = 9), geochemical features that are consistent with high MgO basaltic or picritic, plume-type magmas.

H & E - Hildebrand and Easton 1995, 1997

Reset titanite 12 km S of Grenv F. Krogh 1989 t 982

Re-crystallized NW late shear zone nr Gagnon, Krogh 1989 m 992

French River melt pods, Krogh 1989 z 995

Bayfield Gneiss, Pointe au Baril., Krogh et al. 1993 t 998+15 lower

Parry Sound a boudin of metaseds, Krogh et al. 1993 has newz 1006

French River late pegmatite z 1007

Anorthosite, Riviere Pentecote, Martignole et al. 1993 CJES, t 1008+6

French River late pegmatite r 1016

Grenville Ottawan orogeny

Central Britt shear zonesynkinematic pegmatite z 1019+4

Ductile def in the Bancroft zone Hanmer &McEachern 1992 1030-1000

New z in Algonquin granulite, van Breemen et al. 1986 z 1030+50

*Go Home folded diabase & z 1046

overgrowth z in unstrained anatectic peg of the fold hinge z 1047

Mylonitic Bayfield Gneiss, Pointe au Baril., Krogh et al. 1993 znew 1047

Coronitic metagabbro Davidson and van Breemen z 1047+5

*Go Home folded diabase z 1049

Zircon overgrowths in French River gneiss z 1050

Youngest Moon River attenuated diabase z 1050

Ottawan orogeny, Moore and Thompson 1980, CJES v. 17 1050-1000

Parry Sound, Krogh et al 1993 state met is widespread at 1052

Younger granitoids of the Frontenac cutting upper & lower z 1060 (1080-1060)

Mylonitic Bayfield Gneiss, Pointe au Baril., Krogh et al. 1993 znew 1062

Oldest Moon River attenuated diabase z 1062

Monazite in French River quartzite, Krogh 1989 m 1062

Muskoka mig. ogneiss+leuco. Timmerman etal 1997 z 1064+18 lower 1457+6 upper

Muskoka weakly mig granitoid, Timmerman et al. 1997 z 1066+8 lower1394+13 upper

CMB syntectonic peg., van Breemen and Hanmer 1986 z 1070-1030

Muskoka undef. charnokite vein cutting 1394 deformed z 1077+2

granite in highly deformed gneiss

Ahmic domain overgrowth z in host migmatite z 1078

Muskoka domain amphibolite, Timmerman et al 1997 z 1079+3

Ahmic domain diabase z 1080-1079

Older granitoids of the Frontenac cutting upper & lower pltes z 1080 (1080-1060)

Parry Sound stretch anorth. in N-S shear Krogh et al 1993 newz 1080

Ductile def in the Bancroft zone Hanmer &McEachern 1992 1080-1050

Parry Sound diabase that postdates granulite grade migmat. z 1114+2

Llano uplift post orogenic granite z 1116-1070

Parry Sound sheared amph and anorth. Krogh et al 1993 znew 1116

Keweenawan 1120-1100

Rhyolite and granite clasts in deformed Hazel Fm, Roth 1993 z 1123+29

Abitibi diabase Krogh et al 1987 z 1140.6+_2

Pegmatite leucosomes Krogh and Wardle 1984 z 1150

Morin anorthosite 1159-1126

Boudinaged and foliated pegmatite, van Breemen et al 1986 z 1159

Kingston diabase dikes, post metamorphic see H and E 1995 b 1160

Pegmatite in discrete shear van Breemen et al. 1986 1160-1100

New z in Parry Sound granulite van Breemen et al 1988 z 1161

Supposed thrusting of Frontenac upper plate 1161 (1165-1159)

Youngest granitoids in Frontenac upper plate z 1162 (1179-1162) Nd MA=1.34-1.48

CMB granite, syenite and gabbro plutons, Easton 1986 z 1170-1080

Coronitic metagabbro Davidson & v Breemen 1988 b 1170+30

Oldest granitoid in Frontenac upper plate z 1179 (1179-1162)

Obduction of the Elzevir z 1190-1180

Mercer anorthosite, Prevec & Baadsgaard 1992 z 1222+2

Lavant gabbro of the Elzevir (Frontenac) H and E 1995 z 1225

Bancroft zone gabbros Hanmer & McEachern 1992 z 1230-1180

Elzevir plutons, Heaman et al. 1986 z 1226

Sudbury diabase Krogh et al 1987 z 1238+4

Charnokite in Frontenac upper plate see H and E z 1250

St. Charles anorthosite, Prevec and Baadsgaard 1991 z 1268+20

Grenv SuperGroup volcanics Silver and Lumbers 1966 1286+15

Nobel gneiss, Connare and McNutt 1985 r 1330

Parry Sound sediments, Krogh et al 1993, younger than 1350-1330

Parry Sound marginal orthogneis, van Breemen 1986 z 1346+69

Parry Sound anorthosite, van Breemen et al 1986 z 1350-1450

Anorthosite, Riviere Pentecote, Martignole et al. 1993 CJES z 1354+3

Muskoka weakly mig granitoid, Timmerman et al. 1997 z 1394+13 upper (1066+8)

Cosby granite pegmatite z 1400-1429 Tdm 2.25 D, M. & C 1990

Pegmatite cuts foliation in Killarney porphyry felsite 1400

Cosby granite, Lumbers 1975 z 1400 Tdm 2.25 D, M $ C. 1990

Muskoka granite, Krogh and Davis 1968 z 1414

McKellar gneiss, SE of Whitstone anorth. van Breemen 1986 z 1425+75

Bayfield Gneiss, Pointe au Baril., Krogh et al 1993 t 1430+23 upper

Bayfield Gneiss, Pointe au Baril., Krogh et al. 1993 z 1430+17 lower

Pointe au Baril tonalite, z 1430+17

Pointe au Baril leucosome from the mig mafic supracrustal z 1433+1

Pointe au Baril mig mafic supracrustal, Ketchum et al 1994 z 1452+2

Local melts S of Gren F, Krogh 1989 z tips and titanite tz 1453+7

Britt Domain granite, van Breemen et al. 1986 z 1456+8.5 Tdm 1.81 D, M. & C 1990

Muskoka mig. ogneiss+leuco. Timmerman etal 1997 z 1457+6 upper (1064+18 lower)

Pointe au Baril, unmig. granite, Krogh e tal 1993 z 1458+9 upper (999 Ma lower)

Point au Baril - Shawanaga granites, Ketchum et al 1994 c.1460

Pointe au Baril mig, granite, Krogh 1993 z 1460+5 upper (993 lower)

Muskoka granite, Krogh et al. 1967 r 1465

Algonquin domain metaplutonic rock van Breemen 1986 z 1460+60

Metaplutonic, Lake Muskoka, Krogh et al. 1967 r 1470+10

Bell Lake granite, Van Breemen and Davidson 1988 z 1471+3 Tdm 2.31 D, M. & C 1990

Deformed granite SW GFTZ Krogh and Wardle 1974 z 1550

Killarney Granite Wanless and Loveridge 1972 r 1625

Mattawa quartzite euhed. to rounded z (995 min) Krogh 1989 z 1687+20

French River Granite, Krogh and Davis 1972 r 1689

Beaverstone Bay qtzte zircon needles, Krogh 1989 z 1700

Johnnie Lake granite Krogh et al. 1971 z 1730-

Killarney porphyry Van Breemen and Davidson 1988 z 1732+7

Bayfield Gneiss, Pointe au Baril., Krogh et al. 1993 z 1739+34 upper

Deformed granite SW GFTZ Krogh and Wardle 1974 z 1740

Killarney granite Van Breemen and Davidson 1988 z 1742+1.4 Tdm 2.24,2.28 D, M. & C 1990

Detrital zircon in Fench River gneiss, Krogh 1989 z 1744+11

Jamo Quartzite, detrital zircon z 1885, 2700 Tdm 2.4 D & Mueller manus

Beaverstone Bay qtzte euhedral detrital z, Krogh 1989 z Archean

(20 titanite plot on an Archean - 1062 line)

(22 km S of GF near Hagar, z and t plot on an Archean - 993 line)

French River quartzite, detrital z, Krogh 1989 z Archean

Melt pod 60 km south of GF S of Val d'Or, Krogh 1989 m Archean

b - baddeleyite; z zircon; r - rubidium; m - monazite; t - titanite

    REFERENCES and NOTES

Berman, R.G. , 1991 Thermobarometry using multiequilibrium calculations: a new technique, with petrological applications: Canadian Mineralogist, 29, , 833-855.

Berman, Robert G; Easton, R. Michael; Nadeau, Leopold, 2000. A new tectonometamorphic map of the Canadian Shield; introduction. In: Tectonometamorphic studies in the Canadian Shield (Part II), Berman-Robert-G (editor); Easton-R-Michael (editor); Martin-R-F (editor)
The Canadian Mineralogist. 38, Part 2; Pages 277-285.

Bickford, M.E. Van Schmus, W.R., and Zietz, I., 1986 Proterozoic history of the midcontinent region of North America: Geology, 14, 6, 492-496.

Busch, J.P. Mezger, K., van der Pluijm, B. A., 1997 Suturing and extensional reactivation in the Grenville orogen, Canada: Geology, 25, 6, 507-510.

Corfu, F. and Easton, R.M., 1995 U-Pb geochronology of the Mazinaw terrane, an imbricate segment of the Central Metasedimentary Belt, Grenville Province, Ontario: CJES, 32, 7, 959-976. Easton, R.M. Buckley, S.G., Lobabok, E., and James, R.S., 1999 Grenville - Southern province relationships in Street Township, District of Sudbury: In Report of Field Work and Other Activities . Ontario Geol. Surv. Misc. Paper 166, , 2, 66-69.

Corfu, F. and Easton, R.M., 1997 Sharbot Lake terrane and its relationship to Frontenac terrane, Central Metasedimentary Belt, Grenville Province: new insights from U-Pb geochronology: CJES, 34, 9, 1239-1257.

Corfu, F. and Easton, R.M., 1998 Extension of the Huronian magmatic suite inside the Grenville Province: new zircon U-Pb evidence from the Grenville Front tectonic zone in Street Township, Sudbury region, Ontario: Proceedings of the 44th annual Institute of lake Superior Geology, 44, 2, 59-60.
Synopsis- ultramafic rocks give zircons with same age as the East Bull Lake intrusions

Corrigan, D. , 1990 Geology and U-Pb geochronology of the Key Harbour area, Britt domain, southwest Grenville Province: M.Sc. thesis, Dalhousie University, Halifax, N.S., 168p.

Culshaw, N.G. Corrigan, D., Drage, J., and Wallace, P., 1988 Georgian bay geological synthesis: Key Harbour to Dillon, Grenville Province of Ontario: Current Research, Part C, Geol. Surv. of Canada Paper 88-1C, 129-133.

Culshaw, N.G. et al., 1994 Deep crustal ductile extension following thrusting in the south-western Grenville Province, Ontario: CJES, 31, 1, 160-175.

Cureton, J.S. van der Pluijm, and Essene, E.J., 1997 Nature of the Elzevir - Mazinaw domain boundary, Grenville Orogen, Ontario: CJES, 3, 976-991.

Davidson, A. and Carmichael, D.M. discuss Hildebrand, R.S. and Easton, R.M. reply, 1997 An 1161 suture in the Frontenac terrane, Ontario segment of the Grenville orogen: Geology, 25, 1, 88-89.
Synopsis - maps of Wynne Edwards show that the vast majority of pre-1160 Ma plutons do not contact the marbles, and there are no unambiguous cross cutting relationships. Titanite (Mezger, 1993) in marble ranges from 1157-1178, 4 greater than 1169, all titanites are from the melange and older titanites may be from the upper plate. Melange also met zircon at 1168+3 and titanites at 1159 and 1153 (Corfu, 1995).

Dickin, A.P. and McNutt, R.H., 1989 Nd model age mapping of the southeast margin of the Archean foreland in the Grenville province of Ontario: Geology, 17, 4, 299-302.

Dickin, A.P. McNutt, R.H., and Clifford, P.M., 1990 A neodymium isotope study of plutons near the Grenville Front in Ontario, Canada: Chemical Geology, 83, 315-324.

Dickin, A.P. and McNutt, R.H., 1990 Nd Model-age mapping of Grenville lithotectonic domains: Mid-Proterozoic Crustal Evolution in Ontario: in Gower, C.F., Rivers, C.F., and Ryan, B., eds., Mid- Proterozoic Laurentia - Baltica: Geol. Assoc. Canada, Special Paper 38, 79-94.

Dickin, A.P. and Higgins, M.D., 1992 Sm/Nd evidence for a major 1.5 Ga crust-forming event in the central Grenville Province: Geology, 20, 2, 137-140.

Dickin, A.P. discuss DeWolf, C.P. and Mezger, K., reply, 1995 Comment on "Lead isotope analyses of leached feldspars: constaints on the early crustal history of the Grenville Orogen": Geochimica Cosmochimica Acta, 59, 24, 5233-5234, 5235-5237.

Easton, R.M. , 1992 1992 Friends of the Grenville Workshop: Geos. Can., 19, 1, 38-40.

Easton, R.M. , 1995 Regional geochemical variation in Grenvillian carbonate rocks: implications for mineral exploration: Ontario Geological Survey Miscellaneous Paper 164, Summary of field work and other activies, 1995, 6-18.
Synopsis- breccia marbles are different from low grade marbles of the Frontenac; they have elevated Ti, Zr, ba and Sr

Easton, R.M. , 1996 Project Unit 95-31. Geology of garnetiferous gneisses in Street Township, District of Sudbury: Ontario Geological Survey Miscellaneous Paper 166, Summary of Field Work and Other Activities 1996, , 2, 70-73.

Easton, R.M. , 1997 35. Project Unit 88-05. Regional Mapping and Stratigraphic Studies, Grenville Province: Summary of Field Work and other activities, 1989, Ont. Geol. Surv.; Ont. Geol. Surv. Misc. paper 146, 153-157.

Easton, R.M., Davidson, A., and Murphy, E., 1999 Transects across the Grenville Front near Sudbury, Ontario: Geol. Assoc. Canada, Field Trip A2 Guidebook, , 2, 52 pp.

Easton, R. and Stott, G.M. discuss Parrish, R.R. and Sager-Kinsman, E.A., 1993 Geochronology of detrital zircons from the Elzevir and Frontenac terranes, Central Metasedimentary Belt, Grenville Province, Ontario: CJES, 30, 12, 2523-2525.

Eaton, D.W. Hynes, A., Indares, A., and Rivers. T., 1995 Seismic images of eclogites, crustal-scale extension, and Moho relief in the eastern grenville province, Quebec: Geology, 23, 9, 855-858.

Haggart, M.J. Jamieson, R.A., Reynolds, P.H., Krogh, T.E., Beaumont, C., and Culshaw, N.G., 1993 Last gasp of the Grenville Orogeny: thermochronology of the Grenville Front Tectonic zone near Killarney, Ontario: Jour. Geol., 101, 575-589.

Hanmer, S. and McEachern, S., 1992 Kinematical and rheological evolution of a crustal-scale ductile thrust zone, Central Metasedimentary Belt, Grenville orogen, Ontario: CJES, 29, 8, 1779-1790.
Synopsis- closure of a back arc basin represented by gabbros south of the Bancroft shear zone, in the Elzevir zone

Hanmer-S; Corrigan-David; Pehrsson-S; Nadeau-L 2000. SW Grenville Province, Canada; the case against post-1.4 Ga accretionary tectonics. Tectonophysics. 319; 1, Pages 33-51. 2000.
   AB: Seven accretionary sutures, formed between 1.16 and 1.03 Ga, have been identified by different authors in the Ontario-Quebec-Adirondack (OQA) segment of the Mesoproterozoic Grenville Orogen in Canada. With one exception, the inferred accretionary terrane boundaries lie within, or at the margins of the Central Metasedimentary Belt (CMB), located between the Central Gneiss Belt and the Adirondack Highlands (Central Granulite Terrane). However, geological, geochronological, and petrological data suggest that the Grenville orogen on both sides of the proposed terrane boundaries (sutures) preserves a common 1.4-1.03Ga tectonomagmatic history, inconsistent with its origin as a post-1.4Ga collage of exotic tectonic blocks.
    Features which straddle the proposed 1.16-1.03Ga "sutures", from the Central Gneiss Belt, via the Adirondack Highlands, to the Mauricie area, include; (1) Mesoproterozoic continental crust (1.5-1.4 Ga) forming the host and/or basement to younger magmatic and supracrustal suites. (2) A 1.35-1.3Ga continental arc, remnants of which occur from the CMB boundary zone (CMBBZ) in Ontario to the Appalachians in the United States, built on the 1.5-1.4Ga continental crust. (3) Intrusions of 1.17-1.13 Ga age in the Central Gneiss Belt (mafic suite), and the Adirondack Highlands and their Quebec extension (AMCG suite, i.e. anorthosite massifs and related granitoids). (4) Relics of 1.18-1.14Ga sedimentary basins in the northwestern CMB and the Mauricie area.
    We propose that an alternative model can adequately account for the observed geology of this part of the Grenville orogen wherein, the rocks of the OQA segment were part of an Andean-type margin between 1.4 and 1.2Ga. At 1.35-1.3Ga, a continental magmatic arc was built upon the southeastern margin of Laurentia represented by the 1.5-1.4Ga Mesoproterozoic continental crust. The arc split at 1.3Ga forming an ensialic back arc basin, relics of which now occur in the northwestern part of the CMB, and the back arc basin was flanked to the southeast by an active 1.28-1.25Ga arc. Collision between the Laurentian margin and another continent (Amazonia?) occurred at 1.2 Ga, resulting in closure of the back arc basin and initiation of thrusting along the CMBBZ. Post-collisional lithospheric shortening led to convective removal of thickened subcontinental lithosphere, upper mantle melting, and extension of the overlying crust, resulting in widespread magmatic activity at 1.17-1.13Ga, including emplacement of the AMCG massifs. Crustal extension generated sedimentary basins now represented by the St Boniface sediments in the Mauricie area (1.18 to between 1.15 and 1.09Ga), and the penecontemporaneous Flinton Group in the northwestern CMB. Renewed, post-collisional, granulite facies shortening commenced at 1.12 Ga, manifested as nappes in the Central Gneiss Belt, and thrusting in the Mauricie area. Continued post-collisional shortening at 1.08-1.05 Ga was more localised, resulting in reactivation of thrusting in the CMBBZ, and initiation of the kinematically compatible Tawachiche shear zone along the eastern border of the Quebec extension of the Adirondack Highlands. The characteristics of the OQA segment of the Grenville Orogen can all be accounted for in the context of; (1) a 1.4-1.2Ga, southeast facing Andean-type margin to a Laurentian upper plate, associated with northwest dipping subduction; (2) continental collision at 1.2Ga; and (3) subsequent, continued, post-collisional shortening, without invoking  accretion of exotic terranes between 1.4 and 1.0Ga.

Hildebrand, R.S. and Easton, R.M., 1995 An 1161 Ma suture in the Frontenac terrane, Ontario segment of the Grenville orogen: Geology, 23, 10, 917-920.
Davidson, A. and Carmichael, D.M. discuss Hildebrand, R.S. and Easton, R.M. reply, 1997 An 1161 suture in the Frontenac terrane, Ontario segment of the Grenville orogen: Geology, 25, 1, 88-89.
Synopsis - maps of Wynne Edwards show that the vast majority of pre-1160 Ma plutons do not contact the marbles, and there are no unambiguous cross cutting relationships. Titanite (Mezger, 1993) in marble ranges from 1157-1178, 4 greater than 1169, all titanites are from the melange and older titanites may be from the upper plate. Melange also met zircon at 1168+3 and titanites at 1159 and 1153 (Corfu, 1995).

James, D. T; Kamo, S; Krogh, T. E.,  2000. Preliminary U-Pb geochronological data from the Mealy Mountains Terrane, Grenville
   Province, southern Labrador. Government of Newfoundland and Labrador. Geological Survey.Current Research Report. Pages 169-178.  .
   AB: Preliminary U-Pb geochronological studies of zircon and titanite collected from samples of gneissic monzodiorite, foliated quartz monzodiorite, and an undeformed monzonite that occur in the southwestern part of the Grenvillian Mealy Mountains terrane (MMT) give igneous emplacement ages of 1659 + or - 5 Ma, 1650 + or - 1 Ma and 1643 + or - 2 Ma, respectively. Despite the significant textural and structural differences between the samples, the isotopic data suggest that all three of these pyroxene-bearing granitoid rocks are components of the Mealy Mountains intrusive suite (MMIS), a mid-Labradorian AMCG suite. In contrast, zircons from a sample of foliated granite from the MMT give a 1514 +/ - 10 Ma age, interpreted to be the time of igneous emplacement. This data is significant because it demonstrates that the southwestern MMT includes Pinwarian intrusions, and that it has been overprinted by Mesoproterozoic, post-1514 Ma, deformation. Lower-intercept ages from the two deformed MMIS rocks and the Pinwarian granite are loosely constrained between 1050 and 940 Ma, suggesting the tectonothermal event overprinting these rocks is Grenvillian. However, the data do not eliminate the possibility that the region has been affected by overprinting Paleoproterozoic and Mesoproterozoic events. The fact that the ca. 1643 Ma monzonite is undeformed and has apparently escaped deformation is consistent with field observations that the state-of-strain in the area, at all scales, is heterogeneous, although there is a general increase in both the degree of recrystallization and tectonic fabric development toward the southern MMT.

Ketchum, J.W.F. et al., 1993 U-Pb constraints on the late orogenic extensional and thermal history of the Central Britt shear zone, an allochthon - parautochthon boundary in the Central Gneiss Belt, Ontario: Lithoprobe Abitibi - GrenvilleProject Report no. 33, 161-164.

Ketchum, J.W.F. et al. 1994. 1.45 Ga granulites in the southwestern Grenville province: geologic setting, P-T conditions, and U-Pb geochronology. Geology, 22, 3, 215-218.
    Synopsis: Metamorphism and deformation of orthogneiss and supracrustal gneiss before 1684 Ma was followed by further deformation and metamorphism before 1456 Ma (Corrigan, 1990). Granitic to tonalitic plutons were emplaced throughout the Britt domain at ca. 1460-1430 Ma.
    The low strain area lies immediately north of the Central Britt shear zone, a 3 km thick, northeast- to south-dipping extensional tectonite zone that was active late in the Grenville orogeny. U-Pb data from a late synkinematic pegmatite dike indicate southeast-directed extensional shear at 1010+/- 4 Ma (Ketchum et al. 1993). Rock units lying between this zone and the Parry sound domain lack evidence for pre-Grenvillian events observed in parautochthonous rocks north of the shear zone. This block most likely constitutes a previously unrecognized allochthonous domain (Culshaw et al. 1994). (But shear pod of unfoliated gneiss lies beneath the Shanmugan metagabbro??)
    The low strain area lies within a distinctive structural domain bounded by the Central Britt shear zone and the southeast-dipping Nares Inlet shear zone, which also accomodated southeast directed extension. Outside the the low-strain area in this domain, steep, northeast-striking gneissic foliations and shallowly plunging stretching lineations predominate, in contrast to regional northwest-trending folds and southeast-plunging stretching lineations that generally characterize the Britt domain. Field relations show that northeast-trending fabrics predate development of regional north-west-trending folds and extensional shear zone fabrics, intimating an earlier Grenvillian origin. If extensional shearing and regional folding were coeval (Culshaw et al 1994), decoupling of this crustal block along the boundary shear zones from regional fold deformation may account for the preservation of older structures and mineral assemblages.
    A metabasite pod intrudes the ca 1460 Pointe-au-Baril complex. This body preserves a relict igneous texture, intrusive contacts and primary clinopyroxene. (On the other hand metabasite with cpx bearing cores at Nobel are intimately involved in the fold deformation of the country rock felsic gneisses.)
    Resetting of older zircon to 1433 Ma during Grenvillian met. is considered unlikely given the concordance of the analysis. The Nares inlet shear strikes NE-SW, SE dips SE and has SE extension lineation.

Klemens, W.P. and Schwerdtner, W.M., 1997 Emplacement and deformation of granite pegmatite dykes in a mud-crustal regime of late-orogenic extension, southwest Grenville Province, Ontario, Canada: Geol. Mag., 134, 3, 287-295.

Krogh, T.E. Culshaw, N.G., and Ketchum, J.W.F., 1993 Multiple ages of metamorphism and deformation in the Parry Sound-Pointe au Baril area: Lithoprobe Abitibi - Grenville Project, Report no. 33, 39.

Krogh, T.E. and Wardle, R. 1984. U-Pb isotopic ages along the Grenville Front. Geol. Assoc. Canada Pgm. w. Abst., 9, p. 80p
Synopsis - pre or syn met granites near Killarney = 1740; later cataclastically deformed granite = 1550; Strongly lineated Huronian north of the granites are cut by pegmatites with musc. ages of 1450-1470; near Wanapitei local pegmatoids in the font zone have 1150 zircons . North of North Bay highly met. and deformed gneisses 16 km south of the front are cut by undeformed pegs at 2600; South of Val d'Or 60 km south of the front in the granulite met., zircons from undef. local pegs. are 2600 Ma; northwards increase in met. grade due to uplift of progressively deeper Archean crust to the south; near Lac Jeannien, zircon in metagreywacke. with relic granulite minerals. have Archean age. East of the Labrador Trough sphene, monaz., zircon give a mixing line between 1653 and 993; new zircon growth gives 1645 and 1647 = age of pre-Grenville met.; new zircons in local pegmatoids = 992 = age of most recent metamorphism.

Mader, U.K. and Berman, R.G., 1992 Amphibole thermobarometry: a thermodynamic approach: Current Research: Geological Survey of Canada Paper 92-1E, 393-400.

Nadeau, L. , 1990 Tectonic, thermal and magmatic evolution of the Central Geniss Belt, Huntsville region, southwestern Grenville orogen: Ph.D. thesis, Carleton University, Ottawa, 269p.

Rivard-B; Corriveau-L; Harris-L-B 1999. Structural reconnaissance of a deep crustal orogen using RADARSAT and Landsat
satellite imagery and airborne geophysics.In: Special issue on the applications of RADARSAT-1 data in geology, Singhroy-Vernon-H (prefacer), Canadian Journal of Remote Sensing. 25; 3, Pages 258-267.
   AB: Understanding crustal evolution through studies of highly eroded orogens is a current  scientific challenge worldwide. The marble and quartzite sequences and gneiss complexes of the Mont-Laurier area, in the Central Metasedimentary Belt of Quebec, form a collage of rheologically contrasting lithotectonic domains affected by successive orogenic and magmatic events. Landsat and RADARSAT satellite imagery, with their synoptic view and geomorphic detail, are well suited for the study of structurally complex terrains, especially when image analysis is integrated with regional field and geophysical data. For the Mont-Laurier area, the interpretations of such imagery led to the delineation of intrusive bodies, zones of ductile deformation, and fold interference patterns allowing refinements of existing 1:50 000 maps and providing key information for reconnaissance mapping. The gneiss complexes record early Grenvillian convergence (pre-1.19 Ga) and display a highly contorted distribution of lithologies due to multiple fold interference patterns. On radar and Landsat imagery the complexes are relatively featureless structurally, due to the complex foliation trajectories and the small wavelength of folds. Greater success was obtained for similar structures, in gneisses of the quartzite domain, due to the larger amplitude of folds. Landsat TM band 4 imagery outlines the competency contrast of quartzite versus marble and can be used to map the domain of marble. At 1.165 Ga emplacement of the Chevreuil intrusive suite, concentrated along N-S corridors, marked the onset of renewed orogenic activity. Many of the intrusions from this suite have a unique topographic signature which can be delineated on the Landsat and RADARSAT imagery. Following the magmatic activity, late compressive deformation in the ductile regime was focused along the N-S corridors. The style of this deformation is characterized by a regional N-S foliation and coaxial anastamozing shear zones (NE-SW
dextral; NW-SE sinistral) which were delineated in the radar imagery and confirmed using field kinematic indicators. The RADARSAT imagery provides a view of the extent of this deformation event and corroborates field and petrological studies indicating that by 1.165 Ga, the gneiss complexes were mechanically strong crustal domains and were only locally overprinted by late-stage ductile deformation.

Rivers, T. van Gool, J.A.M., and Connelly, J.N., 1993 Contrasting textonic styles in the northern Grenville province: implications for the dynamics of orogenic fronts: Geology, 21, 12, 1127-1130.

Sharma-Kamal-N-M; Singhroy-Vernon-H; Madore-Louis; Levesque-Josee; Hebert-Claude;  Hinse-Mario 1999. Use of radar images in the identification of major regional structures in the Grenville Province, western Quebec. In: Special issue on the applications of RADARSAT-1 data in geology, Singhroy-Vernon-H (prefacer) Canadian Journal of Remote Sensing. 25; 3, Pages 278-290.
   AB: New structural interpretations result from the remote sensing work carried out in the western part of the Grenville Province in Quebec. Detailed structural interpretation of SEASAT-RADAR images, Airborne-Radar images and RADARSAT images followed by field
observations have led to the recognition of several major geological structures of fundamental importance. The Cayamant Lineament (Cayamant Shear Zone) is significant for several reasons, the most important being that in addition to marking the western limit of the Central Metasedimentay Belt, it also represents a major shear zone resulting from the overthrusting, towards the W and the NW, of the supracrustal pile on top of the adjacent gneissic terranes (Pythonga Terrane and Baskatong-Dozois Terrane). Consequently, the Cayament Lineament defines the eastern limit of the Central Metasedimentary Belt Foreland Zone which extends westward for distances exceeding one hundred kilometres on top of the gneissic terranes. These phenomena are spectacularly evident on the structural interpretations of Radar data. Field studies confirm that these NW trending elliptical structures represent, hitherto unknown, thrust nappes and their erosional remnants. Another major structure identified is the Baskatong-Desert Lineament, which is a steeply dipping to subvertical dextral shear zone, several kilometres thick. It delimits the Baskatong-Dozois Terrane (with Archean Sm/Nd model
ages) to the north, and the Pythonga Terrane (with Proterozoic Sm/Nd model ages) to the south. The Kinonge-Labelle Shear Zone can be  seen to extend northward from the Ottawa River for more than 150 km. Its exposed width exceeds 20 km near the Ottawa River,
whereas in its northern extremity the width is considerably reduced to only a few kilometres. In the eastern part several thrust nappes have also been identified, some of which incorporate the lithologies which are part of the eastern portions of the Morin Anorthosite
Suite. The structural interpretations equally help to constrain the northern limit of the main body of the Central Metasedimentary Belt. The brittle fractures in the southern parts of these areas are related to the Ottawa-Bonnechere and the St. Lawrence Graben Systems. The Radar images have thus been highly useful in outlining most of the structural features previously unknown or only partially known, and not shown on the pre-existing geological maps.

Smith, T.E. and Holm, P.E., 1987 The trace element geochemistry of metavolcanic and dykes from the Central Metasedimentary Belt of the Grenville Province, southeastern Ontario, Canada: Pharaoh, T., Beckinsale, R.D., and Rickard,D.T. eds., Geochemistry and Mineralization of Proterozoic volcanic Suites, Blackwell Sci. Pub., 453-470.
Synopsis - in library at QE461. G353

Timmermann, H. Parrish, R.R., Jamieson, R.A. and Culshaw, N.G., 1997 Time of metamorphism beneath the Central Metasedimentary Belt boundary thrust zone, Grenville Orogen, Ontario: accretion at 1080 Ma?: CJES, 34, 1023-1029.
Synopsis - Baysville , Highw 117, 10 km below the CMBB thrust, igneous protolith of migmatites upper intercept of 1457+7 lower 1064+18; amphibolite = dike 1079+3, absence of inherited zircon. Highway 35 (Minden to Dorset) just west of the CMBB, undeformed opx bearing vein cutting weak to well foliated pink granitoid in strongly deformed migmatitic orthogneisses upper 1077+2, titanite 1065+1 - 1079+1; pink granitoid 1390+85 = crystallization age, lower 1022+109, combined with the vein data upper = 1394+13 lower 1066+8

Tuccillo, M.E. Mezger, K., Essene, E.J., and van der Pluijm, B.A., 1992 Thermobarometry, geochronology and the interpretation of P-T-t data in the Britt domain, Ontario Grenville orogen, Canada: Jour. Petr., 33, 225-1259.

Tucker, R.D. and Gower, C.F A., 1994 U-Pb geochronological framework for the Pinware Terrane, Grenville Province, Southeast Labrador. Jour. Geol., 102, 67-78.
Synopsis - granitoids at 1490+5 and 1479+2, 1472+3; enclaves of supracrustal rocks, incl. felsic volc., at 1640+7; granitoids at 1145; zircon in mafic dike at 1000+2; late granites at 960+2 and 959+2; second of two deformation events assumed to be equivalent to zircon in the mafic diabase; D1 deformation is indicated to be Grenville.

Van Breemen, O., Davidson, A., Loveridge, W.D., and Sullivan, R.W. 1986. U-Pb zircon geochronology of Grenville tectonites, granulites and igenous precursors, Parry Sound, Ontario. In Moore, J.M. et al., eds., The Grenville Province: Geol. Assoc. Canada Spec. paper 31, p. 191-207.

Van Breemen, O. and Davidson, A., 1988 Northeast extension of Proterozoic terranes of mid-continental North America: BGSA, 100, 5, 630-638.

Wasteneys, Hardolph; McLelland, James; Lumbers, Sydney, 1999. Precise zircon geochronology in the Adirondack Lowlands and implications for revising plate-tectonic models of the Central Metasedimentary Belt and Adirondack Mountains, Grenville Province, Ontario and New York. Canadian Journal of Earth Sciences, 36; 6, Pages 967-984.
   AB: New high-precision, single-grain dating of leucogranites from the Adirondack Lowlands, dated previously by multigrain zircon methods at ca. 1416 Ma (Wellesley Island) and ca. 1285-1230 Ma (Hyde School Gneiss), has yielded U-Pb zircon ages of ca. 1172 Ma, identical to that of Rockport granite of the Frontenac terrane. In addition, sensitive high resolution ion microprobe (SHRIMP) zircon dating of the intrusive Antwerp-Rossie suite in the Adirondack Lowlands indicates a maximum emplacement age of ca. 1207 +26/ -11 Ma which fixes a minimum age for deposition of regional metasedimentary rocks that it crosscuts. These results remove apparent chronological discrepancies across the St. Lawrence River, thus expanding the significance of the Rockport granite and Hyde School Gneiss and requiring modification of plate-tectonic models for the Central Metasedimentary Belt and Adirondack  Mountains in the interval ca. 1350-1125 Ma.White, D.J. et al., 1994 Seismic images of the Grenville Orogen in Ontario: CJES, 31, 2, 293-307.

White, J.C. and Flagler, P.A., 1992 Deformation within part of a major crustal shear zone, Parry Sound Ontario: structure and kinematics: CJES, 29, 1, 129-141.

Wodicka, N. and Jamieson, R.A. 1996. The Parry Sound domain: a far-travelled allochthon? New evidence form U-Pb zircon geochronology. CJES, 3, 1087-1104.
Synopsis - basal Parry Sound tonalitic to granitic gneisses - 1400 - 1330; Parry Sound anorthosite - 1163+3; cross-cutting mafic dike - 1151 to 1163; interior Parry Sound assemblage tonalitic gneiss - 1314+12; detrital zircons from quartzite of the basal assemblage range from 1385 to Neoarchean, absolute maximum age of the quartzite is 1436+1. Detrital zircon from the Twelve Mile Bay assemblage sets age of deposition to 1140-1120, are from the Frontenac or Adirondacks. Parry Sound came out of CMBB thrust zone or Adirondack Highlands, emplaced relatively late by about 1080 Ma.

    Canadian Journal of Earth Science Special Issue, Feb/March 2000 - The Lithoprobe Abitibi - Grenville transect

    Corfu-F; Easton-R-M, 2001 U-Pb evidence for polymetamorphic history of Huronian rocks within the Grenville Front  tectonic zone east of Sudbury, Ontario, Canada. In  What are we dating? Understanding the crystallogenesis of U-Pb geochronometers, Scott, David J. (editor); Moser, Desmond E. (editor)  Chemical Geology. 172; 1-2, Pages 149-171.
    AB: This paper presents U-Pb geochronological data for zircon, titanite, monazite, apatite,   allanite, and rutile from Street Township east of Sudbury that help unravel two main facets of the geology of the Grenville Front Tectonic Zone (GFTZ). They document the presence of extensive Huronian Supergroup magmatic (ca. 2480-2460 Ma) and sedimentary rocks inside the GFTZ, and highlight the significance of bimodal magmatism in the genesis of the Huronian Supergroup. The data also provide further insights into the complex orogenic evolution of the GFTZ, showing in particular that amphibolite facies metamorphism, migmatization and   deformation during Grenvillian compression at 995-980 Ma overprinted, but did not totally erase, the memory of earlier metamorphic events at ca. 1720 and 1470 Ma. From the point of view of U-Pb systematics, the results emphasize the nearly ubiquitous state of isotopic disequilibrium in these rocks. Most of the minerals investigated comprise two or more generations and are generally in a state of partial resetting because of the superimposed effects of younger events. The preservation of pre-Grenvillian ages in titanite and allanite demonstrates that processes related to final Grenvillian collision and exhumation occurred at great speed. Only apatite and to some degree rutile yield ages that are clearly post-tectonic, thereby reflecting the final stages of exhumation and cooling of the region.

    Watt-G-R; Kinny-P-D; Friderichsen-J-D 2000 U-Pb geochronology of Neoproterozoic and Caledonian tectonothermal events in the East Greenland Caledonides.Journal of the Geological Society of London. 157, Part 5; Pages 1031-1048
   AB: The East Greenland Caledonides occupy a crucial position in plate-tectonic reconstructions of the Late Mesoproterozoic to Early Neoproterozoic   Grenville-Sveconorwegian belt. We present new field and isotopic data from the northern   Stauning Alper which indicate that the 1050-930 Ma history of the area was characterized by   deposition of extensive clastic sequences. Sources of detritus were dominated by rocks of   Mesoproterozoic age, with only limited contributions from Archaean sources, suggesting   deposition at a distance from the present Caledonian foreland. A Neoproterozoic granite (938+ or -13 Ma) provides evidence for thermal perturbation at a time of extensional collapse and uplift recorded in NW Scotland, the Grenville Belt of Canada, Labrador and the Sveconorwegian of SW Sweden and southern Norway. Widespread anatexis in the northern Stauning Alper at c. 430-425 Ma resulted from both collisional melting and decompression melting on uplift contemporaneous with the early part of orogenic collapse of the Caledonian  Fold Belt. Caledonian deformation was focused at the zone of most extensive granite emplacement. Isotopic evidence suggests that Caledonian granites, previously thought to be entirely post-kinematic, actually predate late Caledonian extension.

Easton-R-M 2000 Tectonic framework of the Precambrian basement of southwestern Ontario revisited. AAPG Bulletin. 84; 9, Pages 1382-1383.
   AB: Precambrian basement in SW Ontario consists of rocks of the Proterozoic Grenville    orogen. Study of drill holes and geophysical data led to subdivision of the basement into    several lithotectonic domains. This paper explores how this subdivision relates to the tectonic    framework of the Grenville proposed by Carr et al. (Can. J. Earth Sci., 2000). Under the new framework, the exposed orogen in Ontario and New York consists of three tectonic elements: 1) pre-Grenvillian Laurentia and its margin with approximately 1740 and 1450 Ma continental arc plutons and supracrustal rocks; 2) Composite Arc Belt of allochthonous approximately 1300-1250 Ma volcanic arcs; and 3) Frontenac-Adirondack Belt of supracrustal and plutonic rocks, of uncertain affinity, that may represent part of the Composite Arc Belt or an offshore (micro)continent. SW Ontario basement consists mainly of rocks of pre-Grenvillian Laurentian
   and its margin, although Composite Arc Belt rocks occur to the east. The Composite Arc and Frontenac-Adirondack belts were amalgamated by approximately 1160 Ma, thrust over Laurentia during approximately 1080-1035 and approximately 1010-980 Ma convergence, and exhumed by <1040 Ma faulting. The relationship between the Midcontinent rift ( approximately 1140-1090 Ma) and Grenville orogenesis is unclear, although the rift likely established a thermal regime that influenced subsequent deformation. Penetrative deformation at approximately 1080-1035 Ma was restricted to rocks of the Laurentian margin and parts of the Composite Arc and Frontenac-Adirondack belts. Deposition of Late Neoproterozoic sediments (e.g., Lake Ontario, Ohio) may reflect Grenville exhumation. Despite a long pre-Grenvillian history, the present crustal architecture and most seismic reflectivity were acquired during 1080-980 Ma tectonism.

Drahovzal-James-A 2000 Alternating extension and contraction in the Proterozoic of the eastern Midcontinent. AAPG Bulletin. 84; 9, Pages 1382
   AB: Previously, the Eastern Granite-Rhyolite Province of the eastern Midcontinent had been understood to be dominantly igneous. Work during the past 10 years has shown that much of the eastern part of the province is actually dominated by sedimentary rocks that are associated with volcanics. Age, stratigraphic, and structural relationships suggest that regionally as many as five major Mesoproterozoic and Neoproterozoic sedimentary sequences have been preserved. Four of these sequences are deposited in rift basins that appear to have been extended between major contractional episodes. The Fort Wayne Rift extensional event (1,325 to 1,284 Ma) was followed by the Elzeverian contraction ( approximately 1,240 to 1,160 Ma). The Midcontinent Rift System extensional event (1,109 to approximately 1,088 Ma) was followed by the Ottawan contraction ( approximately 1,090 to 1,025 Ma) and thrusting in that system. The East Continent Rift Basin extensional event (1,020 to approximately 950 Ma) was followed by the Grenville Front contraction ( approximately 950 to 890 Ma) and folding and faulting in the associated rocks. The last extensional event of the Proterozoic ( approximately 700 to 600 Ma) was followed by the Louisville contraction (600 Ma). The Louisvillle contractional event resulted in thrusting and inversion of the Louisville Block and about 8 km of overburden being removed. West of the Louisville Block during late Mesoproterozoic, foreland basin rocks were deposited in the English Basin and subsequently eroded by a regional unconformity.

Boerner-David-E; Milkereit-Bernd; Davidson-A 2000 Geoscience impact; a synthesis of studies of the Sudbury Structure. Canadian Journal of Earth Sciences,. 37; 2-3, Pages 477-501.
   AB: Geophysical probing results are synthesized into a three-dimensional framework necessary for understanding the genesis of the Sudbury Structure, based primarily on seismic reflection results centred on the Sudbury Igneous Complex. Remnants of crustal melting from a catastrophic meteorite impact are superimposed on the juxtaposition of mid-crustal rocks exhumed during the Archean against deformed Paleoproterozoic sedimentary rocks. Sedimentation, metamorphism, deformation, and metasomatic overprints are all part of the post-impact history of Sudbury and tend to dominate the geophysical response of the structure. Pre-impact deformation, although certainly preserved in some aspects of Sudbury geology, is not clearly expressed in the geophysical data, nor are any elements of
   impact-induced deformation. Geophysical views of the Sudbury Igneous Complex are thus somewhat biased in representing mostly the post-impact, but pre-Grenvillian history of the region, with the exception of igneous events. Establishing the proper context for integrating these geophysical results in the genetic interpretation of the Sudbury Structure depends crucially upon timing constraints.

Rivers-Toby; Corrigan-David 2000. Convergent margin on southeastern Laurentia during the Mesoproterozoic; tectonic implications.
Canadian Journal of Earth Sciences, 37; 2-3, Pages 359-383.
   AB: A continental-margin magmatic arc is inferred to have existed on the southeastern (present coordinates) margin of Laurentia from Labrador to Texas from approximately 1500-1230 Ma, with part of the arc subsequently being incorporated into the 1190-990 Ma collisional Grenville Orogen. Outside the Grenville Province, where the arc is known as the Granite-Rhyolite Belt, it is undeformed, whereas within the Grenville Province it is deformed and metamorphosed. The arc comprises two igneous suites, an inboard, principally quartz monzonitic to granodioritic suite, and an outboard tonalitic to granodioritic suite. The quartz monzonite-granodiorite suite was largely derived from continental crust, whereas the tonalitic-granodiorite suite is calc-alkaline and has a juvenile isotopic signature. Available evidence from the Grenville Province suggests that the arc oscillated between extensional and compressional settings several times during the Mesoproterozoic. Back-arc deposits of several ages, that formed during relatively brief periods of extension, include (1) mafic dyke swarms subparallel to the arc; (2) continental sediments, bimodal volcanics and plateau basalts; (3) marine sediments and volcanics formed on stretched continental crust; and (4) ocean crust in a marginal basin. Closure of the back-arc basins occurred during the accretionary Pinwarian ( approximately 1495-1445 Ma) and Elzevirian ( approximately 1250-1190 Ma) orogenies, as well as during three pulses of crustal shortening associated with the 1190-990 Ma collisional Grenvillian Orogeny. During the Elzevirian Orogeny, closure of the Central Metasedimentary Belt marginal basin in the southeastern Grenville Province was marked by subduction-related magmatism as well as by imbrication of back-arc deposits. The presence of a continental-margin magmatic arc on southeastern Laurentia during the Mesoproterozoic implies that other coeval magmatism inboard from the arc took place in a back-arc setting. Such magmatism was wide-spread and chemically diverse and included large volume "anorogenic" anorthosite-mangerite-charnockite-granite (AMCG) complexes as well as small volume alkaline, quartz-saturated and -undersaturated "within-plate" granitoids. Recognition of the approximately 300 million year duration of the Mesoproterozoic convergent margin of southeastern Laurentia suggests that there may be useful parallels with the evolution of the Andes, which has been a convergent margin since the early Paleozoic.

Hynes-Andrew; Indares-Aphrodite; Rivers-Toby; Gobeil-Andre 2000. Lithoprobe Line 55; integration of out-of-plane seismic results with surface structure, metamorphism, and geochronology, and the tectonic evolution of the eastern Grenville Province. Canadian Journal of Earth Sciences, 37; 2-3, Pages 341-358.
   AB: Lithoprobe line 55, in the Grenville Province of eastern Quebec, provides unusually good  control on the three-dimensional (3-D) geometry and structural relationships among the major lithological units there. Archean basement underlies the exposed Proterozoic rocks, along the entire seismic line, and there is a lateral ramp in this basement immediately behind a lobate stack of thrust slices of high-pressure metamorphic rocks comprising the Manicouagan Imbricate Zone (MIZ). Integration of the 3-D geometry with P-T and geochronological data allows derivation of a tectonic model for the region. The MIZ was buried to depths >60 km at 1050 Ma. Preservation of its high-pressure assemblages, and the absence of metamorphism at 990 Ma, which is characteristic of lower pressure metamorphic rocks that tectonically overlie them, indicates the MIZ rocks were rapidly unroofed, early in the tectonic history. There were two discrete pulses of crustal thickening during the Grenvillian Orogeny in this region. The first, involving imbrication of Labradorian and Pinwarian rocks that comprised part of southeast Laurentia, culminated in the Ottawan pulse at ca. 1050 Ma, and produced the high-pressure metamorphism of the MIZ. Its effects were rapidly reversed, with extrusion of the MIZ rocks to shallow crustal levels at ca. 1020 Ma. The crust was again thickened, with the Moho subsiding to depths >60 km, in the Rigolet pulse at ca. 990 Ma. The site of extrusion of the MIZ was probably controlled by the subsurface lateral ramp. High geothermal gradients indicate that extrusion may have been aided by lithospheric delamination in the crustal-thickening zone.

Corriveau-Louise; van-Breeman-Otto 2000. Docking of the Central Metasedimentary Belt to Laurentia in Geon 12; evidence from the
   1.17-1.16 Ga Chevreuil Intrusive Suite and host gneisses, Quebec. Canadian Journal of Earth Sciences, 37; 2-3, Pages 253-269.
   AB: The Chevreuil intrusive suite (1.17-1.16 Ga) represents a chronological field marker of regional extent that intruded the Central Metasedimentary Belt in the western Grenville Province of Quebec after peak metamorphism. Style and site of magma emplacement, and extent of deformation of Chevreuil plutons and dykes permit unravelling of the early Grenvillian evolution of the belt with respect to cratonal North America. The suite comprises a series of vertically layered gabbro stocks and monzonite-diorite-gabbro sheet intrusions, and a swarm of microdiorite dykes that cut across gneisses. The dykes display systematic variations in extent of deformation across the belt. We targeted U-Pb geochronology on gneisses within the identified strain windows; they preserve the record of a ca. 1.20 Ga high
   pressure-temperature (P-T) metamorphic event. The sheet intrusions define magmatic corridors all along, and concordant with, the western, northern, and eastern tectonic boundaries of the belt. The concordant and elongate shape of these bodies results from emplacement, not deformation. Chevreuil magmas thus sealed the belt boundaries largely in their current positions, with the implication that docking of Elzevirian and pre-Elzevirian terranes with cratonal North America predates 1.17 Ga. We interpret the 1.20 Ga  metamorphism as evidence for the initiation of Grenvillian continent-continent collision during the culmination of the Elzevirian orogeny at ca. 1.22 Ga. Emplacement-related fabrics indicate that the Chevreuil suite and the coeval Morin anorthosite suite intruded during renewed orogenesis. This orogenic pulse (Shawinigan) is not accretionary, but represents a strongly partitioned, compressive, intraplate reactivation event.

Corriveau-Louise; Morin-David 2000. Modelling 3D architecture of western Grenville from surface geology, xenoliths, styles of
   magma emplacement, and Lithoprobe reflectors. Canadian Journal of Earth Sciences, 37; 2-3, Pages 235-251.
   AB: Information derived from regional geology, styles of magma emplacement, xenoliths, and western Grenville Lithoprobe reflectors is integrated to model the architecture of the Central Metasedimentary Belt in Quebec. The belt comprises a thin-skinned western marble domain that projects structurally to the east above a quartzite domain; both domains are underlain by a series of gneiss domes. In contrast, the seismic reflectors dip systematically to the east. They stem from exposed high-strain zones and tectonic boundaries hosting concordant, 1.7-1.16 Ga, postmetamorphic sheetlike plutons. Though discontinuous, the reflectors reach highly reflective crust segments near the Moho. The reflections are interpreted as series of plutons positioning crustal-scale structures rooted in underplated, felsic, and mafic magmas reservoirs. These structures served as magma conduits and ponding sites. The nonreflective segments of the inferred structures are interpreted as through-going pathways for magmas in gneissose crust. Based on the thousands of felsic to ultramafic xenoliths brought up by a 1.07 Ga minette dyke, the nature of the intermediate and lower crust is interpreted as interleaving of nonexposed quartzite-bearing supracrustal assemblages with mylonites, gneisses, and a series of mafic to ultramafic intrusive bodies, many of them inferred to be underplated material. In western Quebec, crustal growth along the pre-Grenvillian Laurentian margin
involved pre-1.2 Ga stacking of allochthons including nonexposed metasedimentary and intrusive components during an early stage of Grenvillian collision. Subsequent, 1.7-1.6 Ga magma emplacement along high-strain zones shaped much of the seismic reflectivity of the
belt.

Ketchum-J-W-F; Davidson-A 2000. Crustal architecture and tectonic assembly of the Central Gneiss Belt, southwestern Grenville Province, Canada; a new interpretation. Canadian Journal of Earth Sciences, 37; 2-3, Pages 217-234.
   AB: The Central Gneiss Belt, southwestern Grenville Province, is characterized by parautochthonous crust in the north and allochthonous lithotectonic domains in the south. Despite nearly two decades of study, the basal decollement to allochthonous domains  transported from the southeast, known as the allochthon boundary thrust, has not been precisely located throughout much of the belt. Between Lake Nipissing and Georgian Bay where its surface trace is known, it separates 1.24 Ga Sudbury metadiabase in the footwall from eclogite remnants and 1.17-1.15 Ga coronitic olivine metagabbro confined to its hanging wall. On the premise that this relationship can be used to trace the allochthon boundary thrust elsewhere in the Central Gneiss Belt, we have sought to extend the known distribution of these mafic rock types, making use of field, petrographic, and geochemical criteria to identify them. New occurrences of all three mafic types are identified in a region extending from south of Lake Nipissing to western Quebec, and the mutually exclusive pattern of occurrence is maintained within this region. Structural trends and reconnaissance mapping of high-strain zones that appear to represent a structural barrier to the mafic suites suggest that the allochthon boundary thrust lies well to the north of its previously suggested location. Our preferred surface trace for it passes around the southern end of the Powassan batholith and through the town of North Bay before turning east to join up with the Lac Watson shear zone in western Quebec. This suggests that a large segment of "parautochthonous" crust lying north of, and including, the Algonquin domain is in fact allochthonous. The mutually exclusive distribution of the mafic suites points to significant separation of allochthonous and parautochthonous components prior to the Grenvillian orogeny, in accord with models of pre-Grenvillian continental rifting proposed by others. Despite a relative abundance of geological and geochronological data for the Central Gneiss Belt and a mafic rock distribution that appears to successfully locate a major tectonic boundary, we emphasize the need for additional field and laboratory work aimed at testing our structural model.

Carr-S-D; Easton-R-M; Jamieson-R-A; Culshaw-N-G 2000. Geologic transect across the Grenville Orogen of Ontario and New York.Canadian Journal of Earth Sciences, 37; 2-3, Pages 193-216.
AB: Revised cross sections of the western Grenville Province incorporate new geologic results and reprocessed seismic reflection data. The geology is presented in terms of three tectonic elements: (1) "pre-Grenvillian Laurentia and its margin" with ca. 1740 and 1450 Ma continental arc plutons and associated supracrustal rocks; (2) "Composite Arc Belt" of allochthonous approximately 1300-1250 Ma volcanic arcs and sedimentary rocks; and (3) "Frontenac-Adirondack Belt" characterized by supracrustal and granitoid rocks, and anorthosites, of uncertain affinity, that may represent a distinctive part of the Composite Arc Belt or an offshore (micro) continent. Rocks of the Composite Arc and Frontenac-Adirondack belts were amalgamated with each other by ca. 1160 Ma, were then thrust over Laurentia during ca. 1080-1035 Ma and ca. 1010-980 Ma phases of convergence, and were dissected and exhumed by <1040 Ma normal faults. Penetrative deformation was restricted to that part of the pre-Grenvillian Laurentian margin that lies to the southeast of the Grenville front and parts of the accreted Composite Arc and Frontenac-Adirondack belts. The Laurentian rocks in the Grenville Province are bounded to the northwest and southeast by southeast-dipping ductile thrust and (or) normal shear zones. The Composite Arc and Frontenac-Adirondack belts to the southeast are bounded by ductile and brittle-ductile thrust and (or) normal faults that separate domains with contrasting cooling histories. Despite a long pre-Grenvillian tectonic and plutonic history, the present crustal architecture and much of the seismic reflectivity were acquired during 1080-980 Ma phases of compression and extension.

White-Donald-J; Forsyth-D-A; Asudeh-I; Carr-S-D; Wu-H; Easton-R-M; Mereu-R F 2000. A seismic-based cross-section of the Grenville Orogen in southern Ontario and western  Quebec. Canadian Journal of Earth Sciences, 37; 2-3, Pages 183-192.
   AB: A schematic crustal cross-section is presented for the southwestern Grenville Province based on reprocessed Lithoprobe near-vertical incidence seismic reflection data and compiled seismic refraction - wide-angle velocity models interpreted with geological constraints. The schematic crustal architecture of the southwest Grenville Province from southeast to northwest comprises allochthonous crustal elements (Frontenac-Adirondack Belt and Composite Arc Belt) that were assembled prior to ca. 1160 Ma, and then deformed and transported northwest over reworked rocks of pre-Grenvillian Laurentia and the Laurentian margin primarily between 1120 and 980 Ma. Reworked pre-Grenvillian Laurentia and Laurentian margin rocks are interpreted to extend at least 350 km southeast of the Grenville Front beneath all of the Composite Arc Belt. Three major structural boundary zones (the Grenville Front and adjacent Grenville Front Tectonic Zone, the Central Metasedimentary Belt boundary thrust zone, and the Elzevir-Frontenac boundary zone) have been identified across the region of the cross-section based on their prominent geophysical signatures comprising broad zones of southeast-dipping reflections and shallowing of mid-crustal velocity contours by 12-15 km. The structural boundary zones accommodated southeast over northwest crustal stacking at successively earlier times during orogeny (ca. 1010-980 Ma, 1080-1060 Ma, and 1170-1160 Ma, respectively). These shear zones root within an interpreted gently southeast-dipping regional decollement at a depth of 25-30 km corresponding to the top of a high-velocity lower crustal layer.

Dickin-A-P  2000 Crustal formation in the Grenville Province; Nd-isotope evidence.  Canadian Journal of Earth Sciences, 37;  2-3, Pages 165-181.
    AB: Ninety-eight new Nd-isotope analyses are presented for gneissic rocks from the Grenville Province. When combined with over 250 published Nd analyses and some unpublished analyses, these data can be used to establish a first-order crustal formation age map for most of the Grenville parautochthon and allochthonous polycyclic belt. In particular,   the geographic extents of a juvenile Labradorian arc (Labradoria) and a juvenile 1.5 Ga arc (Quebecia) are defined, each with an area probably in excess of 100 000 km (super 2) . In addition, pre-1.75 Ga arcs are identified in Ontario (Barilia) and Labrador (Makkovikia). This work largely fills the last major gap in the continent-wide crustal formation age map of the Precambrian Shield of North America.