Sedimentary Basin Classification Table (2011)

Total Page:16

File Type:pdf, Size:1020Kb

Sedimentary Basin Classification Table (2011) GNS Science - Sedimentary Basin Classification Table (2011) geologically defined boundaries of Late Cretaceous summary of basin basin references Neogene character boundaries convenience character type WESTERN BASINS Exon et al. 2004; Wood In NW, part-merge into 1990; Wood & Woodward Minimum sediment isopach on Fairway Basin; in NE, 2002; Stagpoole et al. Cretaceous - Paleogene Challenger Plateau and Lord projection of West Norfolk Intraplate to back-arc 2007; Uruski et al. 2002; Intraplate rift, subsidence intraplate rift; Neogene Taranaki Basin Howe Rise; East Lord Howe Ridge; in S, projection of SE subsiding basin, minor Collot et al. 2009; Exon et and marine trangression intraplate subsidence, Rise Spur; West Norfolk Ridge; Challenger Plateau towards compression in east al. 2007 (but note their minor compression Taranaki Fault. minimum sediment isopach name Aotea Basin not near Cape Foulwind adopted) Minimum sediment isopach W of Cretaceous - Paleogene Bellona Trough and on Lord In east, uncertain Intraplate rift, subsidence intraplate rift; Neogene Bellona Basin Howe Rise; minimum sediment relationship with sequence Intraplate subsiding basin and marine trangression intraplate subsidence, isopach in modern Tasman of Challenger Basin minor compression Basin Monawai Ridge; Lord Howe Cretaceous - Paleogene Rise; minimum sediment Intraplate rift, subsidence intraplate rift; Neogene Monawai Basin Uruski 2010 Intraplate subsiding basin isopach in modern Tasman and marine trangression intraplate subsidence, Basin minor compression Minimum sediment isopach on Cretaceous - Paleogene Uncertain relationships with Wood 1993; Wood & Challenger Plateau Challenger Plateau and Tasman Intraplate rift, subsidence intraplate rifts; Neogene Bellona Basin and West Uruski 2005; Tulloch et al. Intraplate subsiding basin Basin; Alpine Fault and and marine trangression intraplate subsidence, Basins Coast basins 1991 basement outcrop, West Coast minor compression West Norfolk Ridge and Cretaceous - Paleogene prolongation; Norfolk and In SW, projection of West Stagpoole et al. 2009; Northland-Reinga Intraplate rift, subsidence Back-arc subsiding basin, intraplate rift; Neogene Reinga ridges, Vening Meinesz Norfolk Ridge to Waikato Uruski et al. 2008a; Uruski and marine trangression minor compression back-arc subsidence Basin Fracture Zone; Northland coast et al. 2010; Uruski 2009 and/or transpression basement outcrop Cretaceous - Paleogene Waikato, King Taranaki Fault, onshore Edbrooke 2005; Townsend Back-arc subsiding basin, intraplate rifts; Neogene Country and basement outcrop, minimum et al. 2008; Proust et al. minor compression back-arc subsidence sediment isopach 2005 Whanganui Basins and/or transpression Cretaceous - Paleogene Merge west into Challenger Sircombe & Kamp 1998; Intraplate rift, subsidence intraplate rifts; Neogene West Coast Basins On-land basement outcrop Basin or basins, and north Beggs et al. 2008; Beggs et Transform transpressional and marine trangression back-arc subsidence into Taranaki basin al. 2008 and/or transpression Cretaceous - Paleogene Easternmost Alpine Fault trace; Wood et al. 2000; Barnes et intraplate rifts; Neogene Fiordland Basins Puysegur Trench merge to the Transform transpressional al. 2005 back-arc subsidence S; ?merge with Bellona Basin and/or transpression SOUTHERN BASINS Boundary with Great South Onshore Canterbury basement Davey 1977; Mogg et al. Cretaceous - Paleogene Basin taken as Takapu outcrop, Chatham Rise south 2008; Uenzelmann-Neben Intraplate rift, subsidence intraplate rift; Neogene Canterbury Basin Swell and NW-SE oriented Intraplate subsiding basin margin; Campbell Plateau; et al. 2009; Uruski et al. and marine trangression intraplate subsidence, 3000 m total sediment "Takapu Swell" 2007 minor compression isopach Boundary with Canterbury Minimum sediment isopach east Cretaceous - Paleogene taken as Takapu Swell; in of Stewart Island and on Intraplate rift, subsidence intraplate rift; Neogene Great South Basin SE boundary with Pukaki Uruski et al. 2007 Intraplate subsiding basin Campbell Plateau; "Takapu and marine trangression intraplate subsidence, Basin taken as 2000 m total Swell" and prolongation minor compression sediment isopach Cretaceous - Paleogene Minimum sediment isopach on Anderton et al. 1982; Davey Intraplate rift, subsidence intraplate rift; Neogene Campbell Basin Intraplate subsiding basin Campbell Plateau 1990; Cook & Davey 1990 and marine trangression intraplate subsidence, minor compression Cretaceous - Paleogene Outer Campbell Minimum sediment isopach on Davey 1977; Sanford 1980; Intraplate rift, subsidence intraplate rift; Neogene Intraplate subsiding basin Basin Campbell Plateau Davey 1990 and marine trangression intraplate subsidence, minor compression In NE, boundary with Great Cretaceous - Paleogene Minimum sediment isopach on South Basin taken as SW- Sanford 1980; Uruski et al. Intraplate rift, subsidence intraplate rift; Neogene Pukaki Basin Campbell Plateau; minimum Intraplate subsiding basin NE oriented 2000 m total 2007 and marine trangression intraplate subsidence, sediment isopach to seaward sediment isopach minor compression Minimum sediment isopach over Cretaceous - Paleogene In S, merge into modern Western Southland Macquarie Ridge Complex and Intraplate rift, subsidence Transpressional to back- intraplate rifts; Neogene Solander Trough and Turnbull, Uruski et al. 1993 west of Stewart Island; and marine trangression arc back-arc subsidence basins Emerald Basin Southland basement outcrop and/or transpression EASTERN BASINS eastern limit taken as Basement outcrop in East Coast Cretaceous passive modern Hikurangi Trough; ranges; East Cape Ridge; Uruski et al. 2005; Uruski et Passive margin, subsidence margin rift; Neogene East Coast Basin "Uruski Fault" deformation Convergent margin forearc minimum sediment isopach in al. 2006; Uruski et al. 2008b and marine transgression convergent margin front taken as boundary with northern apex; Hikurangi Trough overprint Pegasus Basin Kermadec Ridge, minimum Cretaceous passive Uruski 2008; Uruski et al. sediment isopach in north; East Basement and East Coast Passive margin, subsidence margin rift; Neogene Raukumara Basin 2008b; Sutherland et al. Convergent margin forearc Cape Ridge/margin of East Allochthon outcrop onshore and marine transgression convergent margin 2009 Coast Deformed Belt overprint Three Kings Ridge; a possible Cretaceous passive Northeast Slope minimum sediment isopach to Uncertain relationship with Passive margin, subsidence margin rift; Neogene Herzer et al. 2009 Convergent margin forearc Basin seaward; Colville Ridge; Vening the South Fiji Basin and marine transgression convergent margin Meinesz Fracture Zone overprint Kaikoura Canyon; Hikurangi "Uruski Fault" close to Early Cretaceous Trough; a minimum sediment deformation front taken as Uruski & Jones 2008; Passive margin, subsidence Passive margin, subsidence convergent margin; Late Pegasus Basin isopach on the Hikurangi boundary with East Coast Uruski 2010; Uruski in press and marine transgression and marine transgression Cretaceous to Recent Plateau to the N and E; Basin passive margin Chatham Rise Minimum sediment isopachs to Early Cretaceous Chatham Slope west and north on Hikurangi Davy & Uruski 2002; Davy Passive margin, subsidence Passive margin, subsidence convergent margin; Late Basin Plateau, Wishbone Ridge to the et al. 2008 and marine transgression and marine transgression Cretaceous to Recent E passive margin OLIGOCENE TO RECENT BACK-ARC BASINS Havre Trough - Basement outcrop in southern Taupo Volcanic Zone; Colville Neogene and modern Taupo Volcanic Wright 1993 Back-arc Ridge; Kermadec Ridge; merge back-arc Zone into Lau Basin Norfolk Ridge; a minimum sediment isopach to seaward; Neogene and modern South Norfolk Basin Sdrolias et al. 2004 Back-arc Three Kings Ridge; Vening back-arc Meinesz Fracture Zone Three Kings Ridge, Cook Fracture Zone, Loyalty Ridge, Uncertain relationship with Mortimer et al. 2007; Herzer Oligocene-Miocene back- South Fiji Basin New Hebrides Trench, Hunter Back-arc the South Fiji Basin et al. 2011 arc Fracture Zone, Lau Ridge, Colville Ridge.
Recommended publications
  • Subduction Initiation May Depend on a Tectonic Plate's History 22 June 2021, by David Shultz
    Subduction initiation may depend on a tectonic plate's history 22 June 2021, by David Shultz geological history makes it an ideal location to study how subduction starts. The team's seismic structural analysis showed that subduction zone initiation begins along existing weaknesses in Earth's crust and relies on differences in lithospheric density. The conditions necessary for the subduction zone's formation began about 45 million years ago, when the Australian and Pacific plates started to pull apart from each other. During that period, extensional forces led to seafloor spreading and the creation of new high-density oceanic lithosphere in the south. However, in the north, the thick and buoyant continental crust of Zealandia was merely stretched and slightly thinned. Over the next several million years, the plates rotated, and strike- The Puysegur Trench follows the natural curvature of slip deformation moved the high-density oceanic New Zealand’s South Island, extending southwest from lithosphere from the south to the north, where it the island’s southern tip. Credit: NASA slammed into low-density continental lithosphere, allowing subduction to begin. Subduction zones are cornerstone components of The researchers contend that the differences in plate tectonics, with one plate sliding beneath lithospheric density combined with existing another back into Earth's mantle. But the very weaknesses along the strike-slip boundary from the beginning of this process—subduction previous tectonic phases facilitated subduction initiation—remains somewhat mysterious to initiation. The team concludes that strike-slip might scientists because most of the geological record of be a key driver of subduction zone initiation subduction is buried and overwritten by the because of its ability to efficiently bring together extreme forces at play.
    [Show full text]
  • Vulnerable Marine Ecosystems – Processes and Practices in the High Seas Vulnerable Marine Ecosystems Processes and Practices in the High Seas
    ISSN 2070-7010 FAO 595 FISHERIES AND AQUACULTURE TECHNICAL PAPER 595 Vulnerable marine ecosystems – Processes and practices in the high seas Vulnerable marine ecosystems Processes and practices in the high seas This publication, Vulnerable Marine Ecosystems: processes and practices in the high seas, provides regional fisheries management bodies, States, and other interested parties with a summary of existing regional measures to protect vulnerable marine ecosystems from significant adverse impacts caused by deep-sea fisheries using bottom contact gears in the high seas. This publication compiles and summarizes information on the processes and practices of the regional fishery management bodies, with mandates to manage deep-sea fisheries in the high seas, to protect vulnerable marine ecosystems. ISBN 978-92-5-109340-5 ISSN 2070-7010 FAO 9 789251 093405 I5952E/2/03.17 Cover photo credits: Photo descriptions clockwise from top-left: Acanthagorgia spp., Paragorgia arborea, Vase sponges (images courtesy of Fisheries and Oceans, Canada); and Callogorgia spp. (image courtesy of Kirsty Kemp, the Zoological Society of London). FAO FISHERIES AND Vulnerable marine ecosystems AQUACULTURE TECHNICAL Processes and practices in the high seas PAPER 595 Edited by Anthony Thompson FAO Consultant Rome, Italy Jessica Sanders Fisheries Officer FAO Fisheries and Aquaculture Department Rome, Italy Merete Tandstad Fisheries Resources Officer FAO Fisheries and Aquaculture Department Rome, Italy Fabio Carocci Fishery Information Assistant FAO Fisheries and Aquaculture Department Rome, Italy and Jessica Fuller FAO Consultant Rome, Italy FOOD AND AGRICULTURE ORGANIZATION OF THE UNITED NATIONS Rome, 2016 The designations employed and the presentation of material in this information product do not imply the expression of any opinion whatsoever on the part of the Food and Agriculture Organization of the United Nations (FAO) concerning the legal or development status of any country, territory, city or area or of its authorities, or concerning the delimitation of its frontiers or boundaries.
    [Show full text]
  • Geophysical Structure of the Southern Alps Orogen, South Island, New Zealand
    Regional Geophysics chapter 15/04/2007 1 GEOPHYSICAL STRUCTURE OF THE SOUTHERN ALPS OROGEN, SOUTH ISLAND, NEW ZEALAND. F J Davey1, D Eberhart-Phillips2, M D Kohler3, S Bannister1, G Caldwell1, S Henrys1, M Scherwath4, T Stern5, and H van Avendonk6 1GNS Science, Gracefield, Lower Hutt, New Zealand, [email protected] 2GNS Science, Dunedin, New Zealand 3Center for Embedded Networked Sensing, University of California, Los Angeles, California, USA 4Leibniz-Institute of Marine Sciences, IFM-GEOMAR, Kiel, Germany 5School of Earth Sciences, Victoria University of Wellington, Wellington, New Zealand 6Institute of Geophysics, University of Texas, Austin, Texas, USA ABSTRACT The central part of the South Island of New Zealand is a product of the transpressive continental collision of the Pacific and Australian plates during the past 5 million years, prior to which the plate boundary was largely transcurrent for over 10 My. Subduction occurs at the north (west dipping) and south (east dipping) of South Island. The deformation is largely accommodated by the ramping up of the Pacific plate over the Australian plate and near-symmetric mantle shortening. The initial asymmetric crustal deformation may be the result of an initial difference in lithospheric strength or an inherited suture resulting from earlier plate motions. Delamination of the Pacific plate occurs resulting in the uplift and exposure of mid- crustal rocks at the plate boundary fault (Alpine fault) to form a foreland mountain chain. In addition, an asymmetric crustal root (additional 8 - 17 km) is formed, with an underlying mantle downwarp. The crustal root, which thickens southwards, comprises the delaminated lower crust and a thickened overlying middle crust.
    [Show full text]
  • SEASAT Geoid Anomalies and the Macquarie Ridge Complex Larry Ruff *
    Physics of the Earth and Planetary Interiors, 38 (1985) 59-69 59 Elsevier Science Publishers B.V., Amsterdam - Printed in The Netherlands SEASAT geoid anomalies and the Macquarie Ridge complex Larry Ruff * Department of Geological Sciences, University of Michigan, Ann Arbor, MI 48109 (U.S.A.) Anny Cazenave CNES-GRGS, 18Ave. Edouard Belin, Toulouse, 31055 (France) (Received August 10, 1984; revision accepted September 5, 1984) Ruff, L. and Cazenave, A., 1985. SEASAT geoid anomalies and the Macquarie Ridge complex. Phys. Earth Planet. Inter., 38: 59-69. The seismically active Macquarie Ridge complex forms the Pacific-India plate boundary between New Zealand and the Pacific-Antarctic spreading center. The Late Cenozoic deformation of New Zealand and focal mechanisms of recent large earthquakes in the Macquarie Ridge complex appear consistent with the current plate tectonic models. These models predict a combination of strike-slip and convergent motion in the northern Macquarie Ridge, and strike-slip motion in the southern part. The Hjort trench is the southernmost expression of the Macquarie Ridge complex. Regional considerations of the magnetic lineations imply that some oceanic crust may have been consumed at the Hjort trench. Although this arcuate trench seems inconsistent with the predicted strike-slip setting, a deep trough also occurs in the Romanche fracture zone. Geoid anomalies observed over spreading ridges, subduction zones, and fracture zones are different. Therefore, geoid anomalies may be diagnostic of plate boundary type. We use SEASAT data to examine the Maequarie Ridge complex and find that the geoid anomalies for the northern Hjort trench region are different from the geoid anomalies for the Romanche trough.
    [Show full text]
  • The Age and Origin of Miocene-Pliocene Fault Reactivations in the Upper Plate of an Incipient Subduction Zone, Puysegur Margin
    RESEARCH ARTICLE The Age and Origin of Miocene‐Pliocene Fault 10.1029/2019TC005674 Reactivations in the Upper Plate of an Key Points: • Structural analyses and 40Ar/39Ar Incipient Subduction Zone, Puysegur geochronology reveal multiple fault reactivations accompanying Margin, New Zealand subduction initiation at the K. A. Klepeis1 , L. E. Webb1 , H. J. Blatchford1,2 , R. Jongens3 , R. E. Turnbull4 , and Puysegur Margin 5 • The data show how fault motions J. J. Schwartz are linked to events occurring at the 1 2 Puysegur Trench and deep within Department of Geology, University of Vermont, Burlington, VT, USA, Now at Department of Earth Sciences, University continental lithosphere of Minnesota, Minneapolis, MN, USA, 3Anatoki Geoscience Ltd, Dunedin, New Zealand, 4Dunedin Research Centre, GNS • Two episodes of Late Science, Dunedin, New Zealand, 5Department of Geological Sciences, California State University, Northridge, Northridge, Miocene‐Pliocene reverse faulting CA, USA resulted in short pulses of accelerated rock uplift and topographic growth Abstract Structural observations and 40Ar/39Ar geochronology on pseudotachylyte, mylonite, and other Supporting Information: fault zone materials from Fiordland, New Zealand, reveal a multistage history of fault reactivation and • Supporting information S1 uplift above an incipient ocean‐continent subduction zone. The integrated data allow us to distinguish • Table S1 true fault reactivations from cases where different styles of brittle and ductile deformation happen • Figure S1 • Table S2 together. Five stages of faulting record the initiation and evolution of subduction at the Puysegur Trench. Stage 1 normal faults (40–25 Ma) formed during continental rifting prior to subduction. These faults were reactivated as dextral strike‐slip shear zones when subduction began at ~25 Ma.
    [Show full text]
  • Exploration of New Zealand's Deepwater Frontier * GNS Science
    exploration of New Zealand’s deepwater frontier The New Zealand Exclusive Economic Zone (EEZ) is the 4th largest in the world at about GNS Science Petroleum Research Newsletter 4 million square kilometres or about half the land area of Australia. The Legal Continental February 2008 Shelf claim presently before the United Nations, may add another 1.7 million square kilometres to New Zealand’s jurisdiction. About 30 percent of the EEZ is underlain by sedimentary basins that may be thick enough to generate and trap petroleum. Although introduction small to medium sized discoveries continue to be made in New Zealand, big oil has so far This informal newsletter is produced to tell the eluded the exploration companies. industry about highlights in petroleum-related research at GNS Science. We want to inform Exploration of the New Zealand EEZ has you about research that is going on, and barely started. Deepwater wells will be provide useful information for your operations. drilled in the next few years and encouraging We welcome your opinions and feedback. results would kick start the New Zealand deepwater exploration effort. Research Petroleum research at GNS Science efforts have identified a number of other potential petroleum basins around New Our research programme on New Zealand's Zealand, including the Pegasus Sub-basin, Petroleum Resources receives $2.4M p.a. of basins in the Outer Campbell Plateau, the government funding, through the Foundation of deepwater Solander Basin, the Bellona Basin Research Science and Technology (FRST), between the Challenger Plateau and Lord and is one of the largest research programmes in GNS Science.
    [Show full text]
  • The Gondwana Margin: Proterozoic to Mesozoic
    CORE Metadata, citation and similar papers at core.ac.uk Provided by EPrints Complutense The Gondwana margin: Proterozoic to Mesozoic The longevity and extent of the oceanic southern of '--'H��'.JAJ.J.'u., E. I.M. Gonzalez-Casado and I.A. Dahlquist Gondwana have made it the of intense study for more on "The Maz terrane: a Mesoproterozoic domain in the western than 70 years. It was one of the cradles of terrane and Sierras equivalent to the remains a proving ground for theories of Antofalla block of southern Peru? for West LL.L�""".LE, """'.LJL.LU''-'H and Investigation on this Gondwana evolution" sheds new light on the Middle margin, such as accretionary orogenesis and terrane analysis, is and Late Proterozoic evolution of the western Amazonia margin vital to our understanding of the Proterozoic and Phanerozoic that preceded final amalgamation of West Gondwana in the Late evolution of the continental crust. In this issue of Cambrian. The Maz terrane Gondwana Research, entitled "The West Gondwana Margin: Sierras Pampeanas) is recognised as a new continental terrane Proterozoic to Mesozoic", we have assembled 9 research papers that underwent Grenvillian-age orogeny and was thoroughly various of the evolution of the West the Ordovician Famatinian orogeny. Nd- and Gondwana margin, frrst at the international .L.Ln-''-'�'J.�F. allows correlation of Maz metasedi­ 'Gondwana 12 (Geological and Biological Heritage of Gond- rnp'nt�n"\T rocks with the Mesoproterozoic northern part of the wana)', held in in November 2005. Many -'-'J.�V.L<-"HU craton, of pre-Andean basement in concern southern South which has a continuous southern Peru.
    [Show full text]
  • Developing Community-Based Scientific Priorities and New Drilling
    Workshop Reports Sci. Dril., 24, 61–70, 2018 https://doi.org/10.5194/sd-24-61-2018 © Author(s) 2018. This work is distributed under the Creative Commons Attribution 4.0 License. Developing community-based scientific priorities and new drilling proposals in the southern Indian and southwestern Pacific oceans Robert McKay1, Neville Exon2, Dietmar Müller3, Karsten Gohl4, Michael Gurnis5, Amelia Shevenell6, Stuart Henrys7, Fumio Inagaki8,9, Dhananjai Pandey10, Jessica Whiteside11, Tina van de Flierdt12, Tim Naish1, Verena Heuer13, Yuki Morono9, Millard Coffin14, Marguerite Godard15, Laura Wallace7, Shuichi Kodaira8, Peter Bijl16, Julien Collot17, Gerald Dickens18, Brandon Dugan19, Ann G. Dunlea20, Ron Hackney21, Minoru Ikehara22, Martin Jutzeler23, Lisa McNeill11, Sushant Naik24, Taryn Noble14, Bradley Opdyke2, Ingo Pecher25, Lowell Stott26, Gabriele Uenzelmann-Neben4, Yatheesh Vadakkeykath24, and Ulrich G. Wortmann27 1Antarctic Research Centre, Victoria University of Wellington, Wellington, 6140, New Zealand 2Research School of Earth Sciences, Australian National University, Canberra, 0200, Australia 3School of Geosciences, The University of Sydney, Sydney, NSW2006, Australia 4Alfred Wegener Institute, Helmholtz Center for Polar and Marine Research, 27568 Bremerhaven, Germany 5California Institute of Technology, Pasadena, CA 91125, USA 6College of Marine Science, University of South Florida, Saint Petersburg, FL 33701, USA 7GNS Science, Lower Hutt, 5040, New Zealand 8Japan Agency for Marine-Earth Science and Technology (JAMSTEC), Yokohama 236-0001,
    [Show full text]
  • Paper Is Divided Into Two Parts
    Earth-Science Reviews 140 (2015) 72–107 Contents lists available at ScienceDirect Earth-Science Reviews journal homepage: www.elsevier.com/locate/earscirev Geologic and kinematic constraints on Late Cretaceous to mid Eocene plate boundaries in the southwest Pacific Kara J. Matthews a,⁎, Simon E. Williams a, Joanne M. Whittaker b,R.DietmarMüllera, Maria Seton a, Geoffrey L. Clarke a a EarthByte Group, School of Geosciences, The University of Sydney, NSW 2006, Australia b Institute for Marine and Antarctic Studies, University of Tasmania, TAS 7001, Australia article info abstract Article history: Starkly contrasting tectonic reconstructions have been proposed for the Late Cretaceous to mid Eocene (~85– Received 25 November 2013 45 Ma) evolution of the southwest Pacific, reflecting sparse and ambiguous data. Furthermore, uncertainty in Accepted 30 October 2014 the timing of and motion at plate boundaries in the region has led to controversy around how to implement a Available online 7 November 2014 robust southwest Pacific plate circuit. It is agreed that the southwest Pacific comprised three spreading ridges during this time: in the Southeast Indian Ocean, Tasman Sea and Amundsen Sea. However, one and possibly Keywords: two other plate boundaries also accommodated relative plate motions: in the West Antarctic Rift System Southwest Pacific fi Lord Howe Rise (WARS) and between the Lord Howe Rise (LHR) and Paci c. Relevant geologic and kinematic data from the South Loyalty Basin region are reviewed to better constrain its plate motion history during this period, and determine the time- Late Cretaceous dependent evolution of the southwest Pacific regional plate circuit. A model of (1) west-dipping subduction Subduction and basin opening to the east of the LHR from 85–55 Ma, and (2) initiation of northeast-dipping subduction Plate circuit and basin closure east of New Caledonia at ~55 Ma is supported.
    [Show full text]
  • Proposal to Study Subduction Initiation in Northern Zealandia Tim Stern1
    Proposal to study subduction initiation in northern Zealandia Tim Stern1, Rupert Sutherland2 1 Victoria University of Wellington; 2 GNS Science, Lower Hutt [email protected] Back-arc regions of subduction zones contain sedimentary records that hold clues to the subduction initiation process, and provide complementary insights to fore-arc studies (e.g. Izu-Bonin-Mariana and Tonga). The basins and sedimentary platforms northwest of New Zealand record onset of the Tonga –Kermadec (TK) system during the Eocene- Oligocene (see Gurnis et al. white paper). We propose (mainly) marine geophysical studies that will reveal clues as to how and why TK, and Hikurangi, subduction started. Key features that require study are: Norfolk Ridge (NR); New Caledonia Trough (NCT); Taranaki-Wanganui basins; and Three Kings Ridge (TKR). The NR is where surface convergence was associated with initial subduction. What was the vergence and timing of thrusting, what vertical motions took place, and how do these observations compare and discriminate alternate geodynamic model predictions? The New Caledonia Trough lies adjacent to Norfolk Ridge, was deformed in the subduction initiation event and subsided with large magnitude (Sutherland and al., 2010) that is precisely quantified (1.5 km) at its southern end near the north end of Taranaki Basin (Baur et al., 2013). What was the regional timing of NCT subsidence in relation to other aspects of subduction initiation, and what is its significance? Does the 1.5 km of Oligocene “platform subsidence” seen in oil company drill hole data from South Taranaki Basin at ~ 30 Ma (Stern and Holt, 1994) have a common cause as that in the NCT ? If so, the process occurs on a ~1000 km scale and is clearly geodynamically significant.
    [Show full text]
  • Presentation on Pacific Plate and Associated Boundaries
    PACIFIC PLATE AND ASSOCIATED BOUNDARIES The Pacific Plate • Pacific Plate is the largest plate and an oceanic plate. • It shares its boundaries with numerous plates namely; North American Plate.(Convergent and transform fault) Philippine Plate.(Convergent) Juan de Fuca Plate.(Convergent) Indo – Australian Plate.(Convergent, Transform Fault) Cocos Plate.(Divergent) Nazca Plate.(Divergent) Antarctic Plate.(Divergent,Transform Fault) Types of Plate Boundaries • Convergent Boundary: Subduction zones where two plates converges. Eg; Aleutian Islands(Alaska) • Divergent Boundary: Spreading centres where two plates move away from each other. Eg; East Pacific Rise (MOR, Pacific Ocean). • Transform Faults: Boundary where two plates slide past each other. For Eg. ; San Andreas Fault. BOUNDARY WITH ANTARCTIC PLATE DIVERGENT BOUNDARY • Pacific – Antarctic Ridge TRANSFORM FAULT • Louisville Seamount Chain Pacific – Antarctic Ridge Pacific – Antarctic Ridge(PAR) is located on the seafloor of the South Pacific Ocean. It is driven by the interaction of a mid oceanic ridge and deep mantle plumes located in the eastern portion of East Pacific Ridge. Louisville Seamount Chain It is the longest line of seamount chain in the Pacific Ocean of about 4,300 km, formed along the transform boundary in the western side between Pacific plate and Antarctic plate. It was formed from the Pacific Plate sliding over a long – lived centre of upwelling magma called the Louisville hotspot. BOUNDARY WITH PHILIPPINE PLATE CONVERGENT BOUNDARY • Izu – Ogasawara Trench • Mariana Trench Izu – Ogasawara Trench It is an oceanic trench in the western Pacific Ocean. It stretches from Japan to northern most section of Mariana Trench. Here, the Pacific Plate is being subducted beneath the Philippine Sea Plate.
    [Show full text]
  • 32-1 Arculus.Pdf
    OceTHE OFFICIALa MAGAZINEn ogOF THE OCEANOGRAPHYra SOCIETYphy CITATION Arculus, R.J., M. Gurnis, O. Ishizuka, M.K. Reagan, J.A. Pearce, and R. Sutherland. 2019. How to cre- ate new subduction zones: A global perspective. Oceanography 32(1):160–174, https://doi.org/ 10.5670/oceanog.2019.140. DOI https://doi.org/10.5670/oceanog.2019.140 PERMISSIONS Oceanography (ISSN 1042-8275) is published by The Oceanography Society, 1 Research Court, Suite 450, Rockville, MD 20850 USA. ©2019 The Oceanography Society, Inc. Permission is granted for individuals to read, download, copy, distribute, print, search, and link to the full texts of Oceanography articles. Figures, tables, and short quotes from the magazine may be republished in scientific books and journals, on websites, and in PhD dissertations at no charge, but the materi- als must be cited appropriately (e.g., authors, Oceanography, volume number, issue number, page number[s], figure number[s], and DOI for the article). Republication, systemic reproduction, or collective redistribution of any material in Oceanography is permitted only with the approval of The Oceanography Society. Please contact Jennifer Ramarui at [email protected]. Permission is granted to authors to post their final pdfs, provided byOceanography , on their personal or institutional websites, to deposit those files in their institutional archives, and to share the pdfs on open-access research sharing sites such as ResearchGate and Academia.edu. DOWNLOADED FROM HTTPS://TOS.ORG/OCEANOGRAPHY SPECIAL ISSUE ON SCIENTIFIC OCEAN DRILLING: LOOKING TO THE FUTURE HOW TO CREATE NEW SUBDUCTION ZONES A Global Perspective By Richard J. Arculus, Michael Gurnis, Osamu Ishizuka, Mark K.
    [Show full text]