Reconnaissance geochronology of Baffin Island, N.W.T.

Jackson, George D.; Hunt, P A; Loveridge, W D; Parrish, R. R.

doi:10.4095/129079

Cited by 20 publications

(19 citation statements)

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“…The recognition of the continuous Precambrian geology around northern Baffin Bay is confirmed by the available isotopic ages (Dawes et al, 1988;Frisch and Hunt, 1988;Hegner and Jackson, 1990;Jackson et al, 1990;Schärer andDeutsch, 1990, Jackson andHegner, 1991;Henderson and van Breemen, 1992;Jackson, 2000). This unity also characterises the later Precambrian geology, as shown by the overlying Mesoproterozoic cover sequence (Thule Supergroup) and the Neoproterozoic dyke swarms that pierce it (Dawes, 1997(Dawes, , 2006Oakey, 2005).…”

Section: Disposition Of Precambrian Provinces Around Northern Baffin Baymentioning

confidence: 69%

Palaeoproterozoic and Archaean gneiss complexes in northern Greenland: Palaeoproterozoic terrane assembly in the High Arctic

Nutman

Dawes

Kalsbeek

et al. 2008

Precambrian Research

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Section: Disposition Of Precambrian Provinces Around Northern Baffin Baymentioning

confidence: 69%

Palaeoproterozoic and Archaean gneiss complexes in northern Greenland: Palaeoproterozoic terrane assembly in the High Arctic

Nutman

Dawes

Kalsbeek

et al. 2008

Precambrian Research

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“…2740-2725 Ma Eqe Bay and Isotorq greenstone belts, all of which are intruded by 2726 +3/-2-2658 +16/-14 Ma granodioritic to monzogranitic and rare tonalitic plutonic rocks (Figs. 1 and 2; Jackson et al, 1990;Scott and de Kemp, 1999;Jackson, 2000;Wodicka et al, 2002;Bethune and Scammell, 2003;Scott et al, 2003;Young et al, 2004Young et al, , 2007St-Onge et al, 2005;Johns and Young, 2006). Various felsic plutonic rocks, ranging in age from 1897 +7/-4 to ca.…”

Section: Geological Settingmentioning

confidence: 97%

“…Various felsic plutonic rocks, ranging in age from 1897 +7/-4 to ca. 1805 Ma and including the northernmost components of the post-accretion Cumberland batholith, intrude the Piling Group strata and Archean Rae craton rocks (Jackson et al, 1990;Henderson and Henderson, 1994;Wodicka and Scott, 1997;Scott and Wodicka, 1998;Scott, 1999;Wodicka et al, 2002;this study;Bethune and Scammell, 2003;Gagné et al, 2009;Whalen et al, 2010).…”

Section: Geological Settingmentioning

confidence: 98%

Did a proto-ocean basin form along the southeastern Rae cratonic margin? Evidence from U-Pb geochronology, geochemistry (Sm-Nd and whole-rock), and stratigraphy of the Paleoproterozoic Piling Group, northern Canada

Wodicka

St-Onge

Corrigan

et al. 2014

Geological Society of America Bulletin

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The Paleoproterozoic Piling Group along the southeastern Rae margin, northern Canada, is characterized by thick, deep marine turbidite deposits not observed in timeequivalent, intracratonic basin units further southwest. Models invoked to explain this feature include development of a full-ocean, back-arc, or proto-ocean basin followed by turbidite sedimentation. We present new and existing U-Pb geochronological, Nd isotope, geochemical, and stratigraphic evidence that support a proto-ocean basin model, and we explore the events leading to the formation and closure of such a rift basin during the middle Paleoproterozoic. Sedimentation initiated largely after ca. 2160 Ma with deposition of craton-derived, shallow marine siliciclastic strata (Dewar Lakes formation). Continued extension resulted in accumulation of south-facing carbonate beds (Flint Lake formation) and likely concomitant, arclike tholeiitic to picritic volcanism and voluminous volcani clastic sedimentation (lower Bravo Lake formation) farther outboard at ca. 1980 Ma. Accumulation of intra basinal siliciclastic strata above lower Bravo Lake formation rocks may mark a hiatus in mafi cultramafic magmatism. By ca. 1923 Ma, upper Bravo Lake formation, within-platetype alkaline sill emplacement and vol canism occurred within highly extended crust. The oceanic island basalt-like signatures of the Bravo Lake formation rocks (but lack of depleted, mid-ocean-ridge basalt-type compositions) suggest that by this time the thinned Rae continental lithosphere had fragmented into small crustal block(s) and narrow zone(s) of incipient oceanic crust farther outboard of the Piling Group basin. Rapid subsidence of the southeastern Rae margin ensued, leading to deposition of euxinic (Astarte River formation) and overlying turbiditic strata (Longstaff Bluff formation). The post-ca. 1915 Ma northern turbiditic sedimentary units were likely derived from a thoroughly mixed, two-component source with possible input from the Snowbird tectonic zone and Bravo Lake formation, whereas the post-ca. 1930 Ma southern turbidite unit may have been sourced from the Meta Incognita microcontinent, presently exposed further south. We favor a rift margin over a foreland basin setting for the deposition of the northern turbidite deposits. Subsequent mantle upwelling associated with incipient ocean formation may have triggered melting of highly thinned continental crust resulting in emplacement of latestage, ca. 1897 Ma, contaminated rapakivi granite and highly differentiated mafi c sills. Our results are most consistent, albeit not exclusively, with the much debated model of asthenospheric upwelling and incipient rifting along the Rae-Hearne boundary farther southwest at ca.

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“…However, a subduction-related origin seems at odds with its emplacement into passive margin sequences in both Canada (Piling and Lake Harbour Groups (Jackson et al 1990)) and Greenland (Karrat Group) and is not easily reconciled with emerging tectonic models for West Greenland (van Gool et al 2002;Connelly et al in review). More specifically, the Nagssugtoqidian-Rinkian orogenic system appears to reflect convergence and collision of two cratonic blocks where subduction dipped southwards beneath the North Atlantic craton to produce arc-related magmatism (the Sisimiut and Arfersiorfik intrusive suites) about 500 km south of the PIC (van Gool et al 2002).…”

Section: Introductionmentioning

confidence: 99%

Age, petrogenesis and metamorphism of the syn-collisional Prøven Igneous Complex, West Greenland

Thrane

Baker

Connelly

et al. 2005

Contrib Mineral Petrol

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Age, petrogenesis and metamorphism of the syn-collisional Proven Igneous Complex, West Greenland AbstractThe Paleoproterozoic Prøven Igneous Complex (PIC) in West Greenland extends from ca. 72°15′ to 73°10′N, approximately 500 km north of the subduction-related intrusive complex in the core of the +1100 km wide, asymmetric collisional Nagssugtoqidian-Rinkian Orogen. A new U-Pb SHRIMP age for the PIC of 1869±9 Ma indicates that it intruded synchronously with the main collisional phase of the orogen into the passive margin side of the collision. Sm-Nd and Lu-Hf isotopic and A-type geochemical signatures are compatible with its derivation from melted Archean lower crustal material contaminated to varying degrees by pelitic sedimentary rocks of the Karrat Group. The timing, petrogenesis and position of the PIC within the orogen support a model of collisionally induced delamination of the mantle lithosphere following initial collision. Upwelling asthenospheric mantle replacing the partially or completely detached mantle lithosphere caused widespread partial melting of lower crust that resulted in the areally extensive (∼250,000 km2) CumberlandPrøven intrusive complexes of Baffin Island and West Greenland. Emplacement of the PIC at 1.87 Ga caused a high-temperature low-to medium-pressure metamorphic aureole that contrasts the regional, overprinting higher-pressure amphibolite facies metamorphism. The consequent high-temperature garnet-orthopyroxenebiotite-bearing assemblages occurring within the margin of the intrusion in the aureole are attributed to the intrusion event. Garnet-controlled Sm-Nd and Lu-Hf ages of 1.82-1.80 Ga require efficient diffusion of these elements during orogenic reheating at this time. This age range overlaps the post-collisional, north-south shortening in the Nagssugtoqidian Orogen to the south and serves to confirm the recently proposed genetic link between these two orogens. These new data infer that garnet-controlled isochrons based on the Lu-Hf and Sm-Nd systems cannot date high-grade events in slowly cooled or significantly reheated terrains in rocks possessing other phases that close at low temperatures. © Springer-Verlag 2005. Emplacement of the PIC at 1.87 Ga caused a high-temperature low to medium pressure metamorphic aureole that contrasts the regional, overprinting higher pressure amphibolite facies metamorphism. The consequent high temperature garnet-orthopyroxene-biotite-bearing assemblages occurring within the margin of the intrusion in the aureole is attributed to the intrusion event. Garnet-controlled Sm-Nd and Lu-Hf ages of 1.82-1.80 Ga require efficient diffusion of these elements during orogenic reheating at this time. This age range overlaps the post-collisional, northsouth shortening in the Nagssugtoqidian Orogen to the south and serves to confirm the recentlyproposed genetic link between these two orogens. These new data infer that garnet-controlled isochrons based on the Lu-Hf and Sm-Nd systems cannot date high grade events in slowly-cooled or significantly-reheated ter...

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Reconnaissance geochronology of Baffin Island, N.W.T.

Cited by 20 publications

References 0 publications

Palaeoproterozoic and Archaean gneiss complexes in northern Greenland: Palaeoproterozoic terrane assembly in the High Arctic

Palaeoproterozoic and Archaean gneiss complexes in northern Greenland: Palaeoproterozoic terrane assembly in the High Arctic

Did a proto-ocean basin form along the southeastern Rae cratonic margin? Evidence from U-Pb geochronology, geochemistry (Sm-Nd and whole-rock), and stratigraphy of the Paleoproterozoic Piling Group, northern Canada

Age, petrogenesis and metamorphism of the syn-collisional Prøven Igneous Complex, West Greenland

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