Fore‐arc deformation and underplating at the northern Hikurangi margin, New Zealand

Scherwath, Martin; Kopp, Heidrun; Flueh, Ernst R.; Henrys, S. A.; Sutherland, Rupert; Stagpoole, Vaughan; Barker, D. H. N.; Reyners, Martin; Bassett, Dan; Planert, Lars; Dannowski, Anke

doi:10.1029/2009jb006645

Cited by 37 publications

(74 citation statements)

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“…This process could be the cause of the non-tectonic uplift of 1-1.5 km in the inner zone of ELIP, such as has been suggested by Chen et al (2015). Zealand (Scherwath et al, 2010). Furthermore, numerical simulation of ultramafic magmatic mass intrusion into continental crust (Gerya and Burg, 2007) is also compatible with a very strong density contrast.…”

Section: Crustal Underplatingsupporting

confidence: 57%

Magmatic underplating beneath the Emeishan large igneous province (South China) revealed by the COMGRA-ELIP experiment

et al. 2016

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Section: Crustal Underplatingsupporting

confidence: 57%

Magmatic underplating beneath the Emeishan large igneous province (South China) revealed by the COMGRA-ELIP experiment

et al. 2016

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“…The high topography of the Chugach Range in Alaska, formed 5–10 Ma, has been suggested to result from the entrance of buoyant material (the Yakutat terrane) in the subduction zone [ Abers , 2008]. Another instance of deformation in the overriding plate due to accretionary orogenesis is observed in uplift in the Cape Ridge area and deformation in the forearc of the New Zealand subduction zone, which has been correlated to subduction of the Hikurangi plateau and underplating of a block of sediments [ Scherwath et al , 2010]. …”

Section: Introductionmentioning

confidence: 99%

“…If buoyancy is the main controlling factor, then why are regions of the Ontong Java Plateau, an oceanic plateau with a crustal thickness great enough to resist subduction (33 km) [ Miura et al , 2004], in fact subducting [ Mann and Taira , 2004]? Also, the Hikurangi plateau, an 18 km‐thick oceanic plateau, is seismically imaged to depths of >50 km, subducting intact under New Zealand [ Scherwath et al , 2010; Bassett et al , 2010]. And the Yakutat terrane, currently believed to be an oceanic plateau [ Christeson et al , 2010], has been seismically imaged to depths of ∼130 km [ Eberhart‐Phillips et al , 2006].…”

Section: Introductionmentioning

confidence: 99%

Geodynamic models of terrane accretion: Testing the fate of island arcs, oceanic plateaus, and continental fragments in subduction zones

Tetreault

Buiter

2012

J. Geophys. Res.

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[1] Crustal growth at convergent margins can occur by the accretion of future allochthonous terranes (FATs), such as island arcs, oceanic plateaus, submarine ridges, and continental fragments. Using geodynamic numerical experiments, we demonstrate how crustal properties of FATs impact the amount of FAT crust that is accreted or subducted, the type of accretionary process, and the style of deformation on the overriding plate. Our results show that (1) accretion of crustal units occurs when there is a weak detachment layer within the FAT, (2) the depth of detachment controls the amount of crust accreted onto the overriding plate, and (3) lithospheric buoyancy does not prevent FAT subduction during constant convergence. Island arcs, oceanic plateaus, and continental fragments will completely subduct, despite having buoyant lithospheric densities, if they have rheologically strong crusts. Weak basal layers, representing pre-existing weaknesses or detachment layers, will either lead to underplating of faulted blocks of FAT crust to the overriding plate or collision and suturing of an unbroken FAT crust. Our experiments show that the weak, ultramafic layer found at the base of island arcs and oceanic plateaus plays a significant role in terrane accretion. The different types of accretionary processes also affect deformation and uplift patterns in the overriding plate, trench migration and jumping, and the dip of the plate interface. The resulting accreted terranes produced from our numerical experiments resemble observed accreted terranes, such as the Wrangellia Terrane and Klamath Mountain terranes in the North American Cordilleran Belt.Citation: Tetreault, J. L., and S. J. H. Buiter (2012), Geodynamic models of terrane accretion: Testing the fate of island arcs, oceanic plateaus, and continental fragments in subduction zones,

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“…Bathymetric contours at 1000 m intervals are plotted in red with a digital elevation model (DEM) used to display the Raukumara Peninsula. Red dots denote the locations of Ocean Bottom Seismometers/Hydrophones used in the earlier study of Scherwath et al [2010]. The Kermadec Ridge bounds the western flank of Raukumara Basin.…”

Section: Introductionmentioning

confidence: 99%

Three‐dimensional velocity structure of the northern Hikurangi margin, Raukumara, New Zealand: Implications for the growth of continental crust by subduction erosion and tectonic underplating

Bassett

Sutherland

Henrys

et al. 2010

Geochem Geophys Geosyst

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Traveltimes between shots from nine marine seismic reflection lines and nine onshore recorders were used to construct a 3‐D P wave velocity model of the northern Hikurangi subduction margin, New Zealand. From north to south between Raukumara Basin and Raukumara Peninsula, the Moho of the overriding plate increases in depth from 17 to ∼35 km. Low seismic P wave velocities of 3.5–5.0 km/s are localized within a ∼10 km thick prism in the lower crust of the overriding plate immediately updip of the intersection between the subduction thrust and Moho and beneath the topographic crest of East Cape Ridge and the Raukumara Range. Southward, this region of low seismic velocities and surface uplift increases in distance from the trench as the thickness of the crust in the overriding plate increases. We interpret this low‐velocity volume to be underplated sedimentary rocks and crustal materials that were tectonically eroded by subduction beneath the trench slope. The buoyancy and low strength of these subducted materials are proposed to assist the escape from a subduction channel near the base of the crust and drive local rock uplift. In the middle crust, our observations of very low velocity suggest high fluid‐filled porosities of 12%–18%, and the implied buoyancy anomaly may enhance underplating. At greater depths the process is driven by the contrast between upper crustal quartz‐feldspar mineralogy and the denser diabase or olivine‐rich lithologies of the lower crust and mantle. We estimate a rate of lower crustal underplating at the northern Hikurangi margin of 20 ± 7 km3 Ma−1 km−1 since 22 Ma. We suggest that underplating provides an efficient means of accreting subducted sediment and tectonically eroded material to the lower crust and that the flux of fore‐arc crustal rocks into the mantle at subduction zones may be systematically overestimated.

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Fore‐arc deformation and underplating at the northern Hikurangi margin, New Zealand

Cited by 37 publications

References 100 publications

Magmatic underplating beneath the Emeishan large igneous province (South China) revealed by the COMGRA-ELIP experiment

Magmatic underplating beneath the Emeishan large igneous province (South China) revealed by the COMGRA-ELIP experiment

Geodynamic models of terrane accretion: Testing the fate of island arcs, oceanic plateaus, and continental fragments in subduction zones

Three‐dimensional velocity structure of the northern Hikurangi margin, Raukumara, New Zealand: Implications for the growth of continental crust by subduction erosion and tectonic underplating

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