Landward- and seaward-directed thrusting accompanying the onset of subduction beneath New Zealand

Rait, G. J.; Chanier, Frank; Waters, Donna

doi:10.1130/0091-7613(1991)019<0230:lasdta>2.3.co;2

Cited by 154 publications

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“…Wallace et al [2009] suggested that these paleomagnetic rota- Figure A2. [Ballance, 1976;Rait et al, 1991;Kamp, 1999]. Paleomagnetic data suggest clockwise rotation of the central and southern Hikurangi margin since the early Miocene [Walcott and Mumme, 1982;Mumme and Walcott, 1985;Wright and Walcott, 1986;Thornley, 1996].…”

Section: A212 Mediterraneanmentioning

confidence: 99%

Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Wallace

Ellis

Mann

2009

Geochem Geophys Geosyst

103

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[1] We review geophysical and geological data from 23 active and ancient plate boundaries to document a compelling spatial and temporal relationship between collision, plate boundary curvature, rapid tectonic rotations, and the occurrence of back-arc rifting. Our observations support a conceptual model where the change from subduction to collision causes rapid fore-arc rotation (when viewed in a reference frame relative to the bounding tectonic plates), leading to marked plate boundary curvature. Our global compilation reveals that most active back-arc rifts are associated with rapidly rotating fore arcs and nearby collisions. Thus, we propose that collision and rapid fore-arc rotations play a major role in the evolution and kinematics of back-arc basins. We conduct numerical modeling to better understand the physical processes behind these observed rapid tectonic rotations at convergent margins. Our results suggest that the presence of an indentor or choke point in the subduction system (e.g., collision) can generate rapid rotation of the fore arc about a nearby pole and lead to back-arc rifting. The rate of fore-arc rotation and back-arc rifting depends on the incoming indentor velocity and can be greatly enhanced by slab rollback and the presence of a low-viscosity back arc. Where viscosity of the back arc is low, fore-arc rotation dominates; where back-arc viscosity is high, the formation of strike-slip faults and tectonic escape dominates. Our observational and model-derived results illustrate that shallow crustal forces produced by the entry of buoyant features into subduction zones are a fundamental mechanism for the generation of fore-arc block rotations, plate boundary curvature, back-arc rift evolution, and tectonic escape in subduction systems. Rollback of the subducting slab within the mantle will certainly enhance the processes we describe but it is not the only driving force. Wallace, L. M., S. Ellis, and P. Mann (2009), Collisional model for rapid fore-arc block rotations, arc curvature, and episodic back-arc rifting in subduction settings, Geochem. Geophys. Geosyst., 10, Q05001,

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Section: A212 Mediterraneanmentioning

confidence: 99%

Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Wallace

Ellis

Mann

2009

Geochem Geophys Geosyst

103

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“…Although the major faults arc primarily strike-slip, the lesser vertical component has been sufficient to form large tilt blocks, such that the late Mesozoic and Cenozoic cover strata are preserved only on the downthrown sides of the major faults, and east and northeast of the terminations of the Hope and Clarence Faults. Numerous fault and fold structures have been mapped within the cover strata (Lensen 1962;Prebble 1980;Kirkei 1989;Rait et al 1991 ), and Carter & Carter ( 1982) and Lewit -& Bennett (1985) have made preliminary compilations ol offshore structures (Fig. 1).…”

Section: Introductionmentioning

confidence: 99%

Pleistocene coastal terraces of Kaikoura Peninsula and the Marlborough coast, South Island, New Zealand

Ôta

Pillans

Berryman

et al. 1996

New Zealand Journal of Geology and Geophysics

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“…1) commenced during the early Miocene (Ballance 1976;Rait et al 1991) and is presently associated with a relative plate motion vector of c. 38-50 mm/yr, trending at c. 40-70° to the strike of the margin (DeMets et al 1994). Numerous geologic, geodetic, and seafloor spreading studies constrain the evolution of the margin and help us to better understand the way in which oblique subduction of the Pacific plate is expressed in the overriding Australian plate (e.g., Walcott 1978;Pettinga 1982;Cashman et al 1992; Lewis & Pettinga 1993;DeMets et al 1994;Darby & Meertens 1995;Kelsey et al 1995;Lamarche et al 1995).…”

Section: Introductionmentioning

confidence: 99%

Structure and deformational history of the inner forearc region, Hikurangi subduction margin, New Zealand

Beanland

Melhuish

Nicol

et al. 1998

New Zealand Journal of Geology and Geophysics

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Seismic reflection and outcrop data from the onshore Hikurangi forearc reveal the styles and history of deformation for a c. 3000 km 2 region between Dannevirke and Hawke' s Bay. The data cover the forearc basin, including its western and eastern boundaries, and delineate folds and faults in a late Miocene-Recent sedimentary sequence. Five seismic horizons, including the basement/Neogene cover unconformity (variable age), base Waipipian (3.7 Ma), base Mangapanian (3.2 Ma), base Nukumaruan (2.6 Ma), and base Castlecliffian (1.6 Ma) were identified using outcrop and well ties. These horizons were traced across the study region to provide information on the geometry, spatial distribution, and timing of structures. To the west, the rangefront fault is predominantly reverse and separates uplifted Torlesse basement of the axial ranges from Neogene forearc basin sediments. Structures within the forearc basin are dominated by north-northeast-striking reverse faults and associated asymmetric folds which parallel the subduction margin and often have sinuous traces. Faults are planar to depths of at least 1-2 km and typically dip at 30-80°NW (most often at 40-70°). Many faults in the basin terminate northwards and fault-normal spacings decrease from 2-8 km in the Dannevirke area to c. 20 km near Hastings. Angular unconformities and syntectonic strata constrain the timing of deformation on fault/fold pairs. Faults within the forearc basin were active over two main periods, at c. ?3.1-2.5 Maandc. 1.6 Ma-Recent. Active fault traces are confined to the edges of the forearc basin. In the west, the Mohaka and Ruahine Faults have mainly recent right-lateral offsets, but interpretation of a seismic reflection line which crosses the Mohaka Fault indicates minimal (<300 m) right-lateral displacement over the last 3 m.y., and lateral slip may not significantly predate the late Quaternary. In the east, a zone of reverse faults (including the Longlands, Poukawa, Tukituki, and Oruawharo Faults) began forming ate. 1 Ma and remains active. Margin-normal shortening across the forearc basin and basin-bounding structures ranges up to 5 mm/yr (120- *

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Landward- and seaward-directed thrusting accompanying the onset of subduction beneath New Zealand

Cited by 154 publications

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Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Collisional model for rapid fore‐arc block rotations, arc curvature, and episodic back‐arc rifting in subduction settings

Pleistocene coastal terraces of Kaikoura Peninsula and the Marlborough coast, South Island, New Zealand

Structure and deformational history of the inner forearc region, Hikurangi subduction margin, New Zealand

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