Evidence from neodymium isotopes for mantle contributions to Phanerozoic crustal genesis in the Canadian Cordillera

Samson, Scott D.; McClelland, William C.; Patchett, P. Jonathan; Gehrels, George E.; Anderson, Robert

doi:10.1038/337705a0

Cited by 163 publications

(88 citation statements)

References 32 publications

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“…It is widely accepted that the formation of the continental crust was essentially complete in the Precambrian (Condie, 1998;Taylor and McLennan, 1995). However, in recent decades, this idea was challenged by isotope investigations in western North America (Sierra Nevada, Peninsular Range, and Canadian Cordillera) (Lee et al, 2007;Samson et al, 1989), South America (Andean) (Mišković and Schaltegger, 2009), eastern Australia (Lachlan and New England Fold belts) (Collins, 1998;McCulloch and Chappell, 1982), the central Asian Orogenic Belt (also known as the Altaid Tectonic Collage) (e.g., Jahn, 2004;Kröner et al, 2014;Sengör et al, 1993) and south Tibet (Gangdese belt) (e.g., Chu et al, 2006;Ji et al, 2009;Ma et al, 2013a;Mo et al, 2008;Zhang et al, 2014c;Zhu et al, 2011), which revealed that a substantial proportion of Phanerozoic crust is juvenile. Phanerozoic continental crustal growth primarily occurs in subduction zones by lateral accretion of island or intra-oceanic arc complexes and oceanic plateaus or by vertical addition by underplating of basaltic magmas in the crust-mantle interface (Chen and Arakawa, 2005;Jahn, 2004;Rudnick, 1995).…”

Section: Introductionmentioning

confidence: 99%

Underplating of basaltic magmas and crustal growth in a continental arc: Evidence from Late Mesozoic intermediate–felsic intrusive rocks in southern Qiangtang, central Tibet

Hao

Wang

Wyman

et al. 2016

Lithos

131

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Section: Introductionmentioning

confidence: 99%

Underplating of basaltic magmas and crustal growth in a continental arc: Evidence from Late Mesozoic intermediate–felsic intrusive rocks in southern Qiangtang, central Tibet

Hao

Wang

Wyman

et al. 2016

Lithos

131

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“…Thus, accretionary orogens, with their subductionrelated plate margins, are seen as the sites of net continental growth, rather than collisional orogens, which are envisaged as sites of crustal reworking (Dewey et al 1986). Geochemical and isotopic studies from Neoproterozoic to Phanerozoic accretionary orogens in the Arabian -Nubian Shield, the Canadian Cordillera and the Central Asian Orogenic Belt indicate massive addition of juvenile crust during the period of 900-100 Ma (Samson et al 1989;Kovalenko et al 1996;Jahn et al 2000a;Wu et al 2000;Jahn 2004;Stern in press). However, recent whole-rock Nd and zircon Hf( -O) isotope data imply that continental crust formation was episodic, with significant pulses of juvenile magmatism and crustal growth in the Archaean and Palaeoproterozoic, and with no significant addition in the Phanerozoic ( Fig.…”

Section: Accretionary Orogens and Continental Growthmentioning

confidence: 99%

“…Western North America is composed of a series of accreted oceanic domains (Coney et al 1980;Samson et al 1989;Fuis & Mooney 1990;Fuis 1998;Fuis et al 2008). A detailed seismic transect from the active plate boundary at the Aleutian Trench in the Gulf of Alaska to the orogenic foreland fold-and-thrust belt on the margin of the Arctic Ocean shows a history of continental growth through magmatism, accretion and underplating (Fuis & Plafker 1991;Fuis et al 2008;Fig.…”

Section: Western Margin Of North Americamentioning

confidence: 99%

Accretionary orogens through Earth history

et al. 2009

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Accretionary orogens form at intraoceanic and continental margin convergent plate boundaries. They include the supra-subduction zone forearc, magmatic arc and back-arc components. Accretionary orogens can be grouped into retreating and advancing types, based on their kinematic framework and resulting geological character. Retreating orogens (e.g. modern western Pacific) are undergoing long-term extension in response to the site of subduction of the lower plate retreating with respect to the overriding plate and are characterized by back-arc basins. Advancing orogens (e.g. Andes) develop in an environment in which the overriding plate is advancing towards the downgoing plate, resulting in the development of foreland fold and thrust belts and crustal thickening. Cratonization of accretionary orogens occurs during continuing plate convergence and requires transient coupling across the plate boundary with strain concentrated in zones of mechanical and thermal weakening such as the magmatic arc and back-arc region. Potential driving mechanisms for coupling include accretion of buoyant lithosphere (terrane accretion), flat-slab subduction, and rapid absolute upper plate motion overriding the downgoing plate. Accretionary orogens have been active throughout Earth history, extending back until at least 3.2 Ga, and potentially earlier, and provide an important constraint on the initiation of horizontal motion of lithospheric plates on Earth. They have been responsible for major growth of the continental lithosphere through the addition of juvenile magmatic products but are also major sites of consumption and reworking of continental crust through time, through sediment subduction and subduction erosion. It is probable that the rates of crustal growth and destruction are roughly equal, implying that net growth since the Archaean is effectively zero.Classic models of orogens involve a Wilson cycle of ocean opening and closing with orogenesis related to continent-continent collision. These imply that mountain building occurs at the end of a cycle of ocean opening and closing, and marks the termination of subduction, and that the mountain belt should occupy an internal location within an assembled continent (supercontinent). The modern Alpine -Himalayan chain exemplifies the features of this model, lying between the Eurasian and colliding African and Indian plates (Fig.

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“…186 Ma plutons intrude and stitch together Stikinia-Quesnellia and the pericratonic terranes [41], limiting imbrication to the Early Jurassic or earlier. A magmatic arc (Stuhini-Nicola) consisting of isotopically juvenile mafic volcanic rocks [42], that developed on Stikinia-Quesnellia (and on the previously accreted Cache Creek seamounts) in the Upper Triassic contrasts with coeval quiescence in the pericratonic belt, implying separation of these terranes until the end of the Triassic. The Stuhini-Nicola arc probably provides a record of closure of an oceanic basin separating Stikinia-Quesnellia and the pericratonic belt, with final closure and collision occurring in the latest Triassic-earliest Jurassic.…”

Section: Pericratonic Beltmentioning

confidence: 99%

The odyssey of the Cache Creek terrane, Canadian Cordillera: Implications for accretionary orogens, tectonic setting of Panthalassa, the Pacific superwell, and break-up of Pangea

Johnston

Borel²

2007

Earth and Planetary Science Letters

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The Cache Creek terrane (CCT) of the Canadian Cordillera consists of accreted seamounts that originated adjacent to the Tethys Ocean in the Permian. We utilize Potential Translation Path plots to place quantitative constraints on the location of the CCT seamounts through time, including limiting the regions within which accretion events occurred. We assume a starting point for the CCT seamounts in the easternmost Tethys at 280 Ma. Using reasonable translation rates (11 cm/a), accretion to the StikiniaQuesnellia oceanic arc, which occurred at about 230 Ma, took place in western Panthalassa, consistent with the mixed Tethyan fauna of the arc. Subsequent collision with a continental terrane, which occurred at about 180 Ma, took place in central Panthalassa, N 4000 km west of North America yielding a composite ribbon continent. Westward subduction of oceanic lithosphere continuous with the North American continent from 180 to 150 Ma facilitated docking of the ribbon continent with the North American plate.The paleogeographic constraints provided by the CCT indicate that much of the Canadian Cordilleran accretionary orogen is exotic. The accreting crustal block, a composite ribbon continent, grew through repeated collisional events within Panthalassa prior to docking with the North American plate. CCT's odyssey requires the presence of subduction zones within Panthalassa and indicates that the tectonic setting of the Panthalassa superocean differed substantially from the current Pacific basin, with its central spreading ridge and marginal outward dipping subduction zones. A substantial volume of oceanic lithosphere was subducted during CCT's transit of Panthalassa. Blanketing of the core by these cold oceanic slabs enhanced heat transfer out of the core into the lowermost mantle, and may have been responsible for the Cretaceous Normal Superchron, the coeval Pacific-centred mid-Cretaceous superplume event, and its lingering progeny, the Pacific Superswell. Far field tensile stress attributable to the pull of the slab subducting beneath the ribbon continent from 180 to 150 Ma instigated the opening of the Atlantic, initiating the dispersal phase of the supercontinent cycle by breaking apart Pangea. Docking of the ribbon continent with the North American plate at 150 Ma terminated the slab pull induced stress, resulting in a drastic reduction in the rate of spreading within the growing Atlantic Ocean.

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Evidence from neodymium isotopes for mantle contributions to Phanerozoic crustal genesis in the Canadian Cordillera

Cited by 163 publications

References 32 publications

Underplating of basaltic magmas and crustal growth in a continental arc: Evidence from Late Mesozoic intermediate–felsic intrusive rocks in southern Qiangtang, central Tibet

Underplating of basaltic magmas and crustal growth in a continental arc: Evidence from Late Mesozoic intermediate–felsic intrusive rocks in southern Qiangtang, central Tibet

Accretionary orogens through Earth history

The odyssey of the Cache Creek terrane, Canadian Cordillera: Implications for accretionary orogens, tectonic setting of Panthalassa, the Pacific superwell, and break-up of Pangea

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