Backarc rifting, constructional volcanism and nascent disorganised spreading in the southern Havre Trough backarc rifts (SW Pacific)
Identifieur interne : 000094 ( PascalFrancis/Corpus ); précédent : 000093; suivant : 000095Backarc rifting, constructional volcanism and nascent disorganised spreading in the southern Havre Trough backarc rifts (SW Pacific)
Auteurs : Rj. Wysoczanski ; E. Todd ; I. C. Wright ; M. I. Leybourne ; J. M. Hergt ; C. Adam ; K. MackaySource :
- Journal of volcanology and geothermal research [ 0377-0273 ] ; 2010.
Descripteurs français
- Pascal (Inist)
- Rifting, Volcanisme, Fossé, Haute résolution, Seabeam, Collection, Submersible, Modèle, Magmatisme, Subduction, Plaque Australienne, Limite plaque, Foyer, Mont sous marin, Graben, Profondeur, Ecoulement, Croûte terrestre, Basalte olivine, Andésite basaltique, Morphologie, Bilan masse, Epaisseur, Atténuation, Accrétion, Bassin Lau.
English descriptors
- KwdEn :
- Australian Plate, Lau Basin, Seabeam, accretion, attenuation, basaltic andesite, collections, crust, depth, flow, focus, grabens, high resolution, magmatism, mass balance, models, morphology, olivine basalt, plate boundaries, rifting, seamounts, subduction, submersibles, thickness, troughs, volcanism.
Abstract
High resolution multibeam (EM300 and SEABEAM) data of the Southern Havre Trough (SHT), combined with observations and sample collections from the submersible Shinkai6500 and deep-tow camera, are used to develop a model for the evolution and magmatism of this backarc system. The Havre Trough and the associated Kermadec Arc are the product of westward subduction at the Pacific-Australian plate boundary. Detailed studies focus on newly discovered features including a seamount (Saito Seamount) and a deep graben (Ngatoroirangi Rift, >4000 m water depth floored with a constructional axial volcanic ridge > 5 km in length and in excess of 200 m high), both of which are characterised by pillow and lobate flows estimated at <20,000 years old based on sediment cover, high reflectivity and thin Mn crusts on recovered glassy olivine basalts and basaltic andesites. Elongate volcanic ridges at 35°15'S and 34°30'S, and backarc seamounts (35°30'S,178°30'E) occur at the eastern margin of the SHT. Similar seafloor morphology is observed in the central and western portions of the basin, suggesting that recent volcanism may be broadly distributed across the backarc. Mass balance modelling indicates a maximum crustal thickness of ˜11 km to <6 krn, similar to estimates of crustal thickness in the Lau Basin to the north. Given such high crustal attenuation and extensive backarc mafic magmatism within deep SHT rifts, we propose that the SHT is in an incipient phase of distributed and "disorganised" oceanic crustal accretion in multiple, ephemeral, and short but deep (>4000 m) spreading systems. These discontinuous spreading systems are characterised by failed rifts, rift segmentation, and propagation. Successive episodes of magmatic intrusion into thinned faulted arc basement results in defocused asymmetrical accretion. Cross-arc volcanic chains, isolated volcanoes and underlying basement plateaus are interpreted to represent a "cap" of recent extrusives. However, they may also be composed entirely of newly accreted crust and the spatially extensive basement fabric of elongated volcanic ridges may be the surface expression of pervasive dike intrusion that has thoroughly penetrated and essentially replaced the original arc crust with newly accreted intrusives.
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Pour connaître la documentation sur le format Inist Standard.
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Format Inist (serveur)
| NO : | PASCAL 10-0252673 INIST |
|---|---|
| ET : | Backarc rifting, constructional volcanism and nascent disorganised spreading in the southern Havre Trough backarc rifts (SW Pacific) |
| AU : | WYSOCZANSKI (Rj.); TODD (E.); WRIGHT (I. C.); LEYBOURNE (M. I.); HERGT (J. M.); ADAM (C.); MACKAY (K.); WYSOCZANSKI (Richard J.); ROWLAND (Julie V.); BEKER (Joel A.); WILSON (Colin J. N.) |
| AF : | Japan Agency for Marine Earth Science and Technology/Yokosuka, 237-0061/Japon (1 aut., 6 aut.); Department of Earth and Planetary Sciences, University of California, Santa Cruz, 1156 High St./Santa Cruz, CA, 95064/Etats-Unis (2 aut.); National Oceanography Centre, Southampton, Empress Dock/European Way, Southampton SO14 3ZH/Royaume-Uni (3 aut.); Ocean Exploration, GNS Science/30-368, Lower Hutt/Nouvelle-Zélande (4 aut.); School of Earth Sciences, The University of Melbourne/VIC 3010/Australie (5 aut.); National Institute of Water and Atmospheric Research/14-901, Wellington/Nouvelle-Zélande (7 aut.); National Institute of Water and Atmospheric Research, Private Bag 14901/Wellington 6041/Nouvelle-Zélande (1 aut.); School of Geography, Environment and Earth Sciences, Victoria University of Wellington, PO Box 600/Wellington 6041/Nouvelle-Zélande (1 aut., 3 aut., 4 aut.); School of Environment, University of Auckland, Private Bag 92019/Auckland 1142/Nouvelle-Zélande (2 aut.) |
| DT : | Publication en série; Niveau analytique |
| SO : | Journal of volcanology and geothermal research; ISSN 0377-0273; Coden JVGRDQ; Royaume-Uni; Da. 2010; Vol. 190; No. 1-2; Pp. 39-57; Bibl. 1 p.1/2 |
| LA : | Anglais |
| EA : | High resolution multibeam (EM300 and SEABEAM) data of the Southern Havre Trough (SHT), combined with observations and sample collections from the submersible Shinkai6500 and deep-tow camera, are used to develop a model for the evolution and magmatism of this backarc system. The Havre Trough and the associated Kermadec Arc are the product of westward subduction at the Pacific-Australian plate boundary. Detailed studies focus on newly discovered features including a seamount (Saito Seamount) and a deep graben (Ngatoroirangi Rift, >4000 m water depth floored with a constructional axial volcanic ridge > 5 km in length and in excess of 200 m high), both of which are characterised by pillow and lobate flows estimated at <20,000 years old based on sediment cover, high reflectivity and thin Mn crusts on recovered glassy olivine basalts and basaltic andesites. Elongate volcanic ridges at 35°15'S and 34°30'S, and backarc seamounts (35°30'S,178°30'E) occur at the eastern margin of the SHT. Similar seafloor morphology is observed in the central and western portions of the basin, suggesting that recent volcanism may be broadly distributed across the backarc. Mass balance modelling indicates a maximum crustal thickness of ˜11 km to <6 krn, similar to estimates of crustal thickness in the Lau Basin to the north. Given such high crustal attenuation and extensive backarc mafic magmatism within deep SHT rifts, we propose that the SHT is in an incipient phase of distributed and "disorganised" oceanic crustal accretion in multiple, ephemeral, and short but deep (>4000 m) spreading systems. These discontinuous spreading systems are characterised by failed rifts, rift segmentation, and propagation. Successive episodes of magmatic intrusion into thinned faulted arc basement results in defocused asymmetrical accretion. Cross-arc volcanic chains, isolated volcanoes and underlying basement plateaus are interpreted to represent a "cap" of recent extrusives. However, they may also be composed entirely of newly accreted crust and the spatially extensive basement fabric of elongated volcanic ridges may be the surface expression of pervasive dike intrusion that has thoroughly penetrated and essentially replaced the original arc crust with newly accreted intrusives. |
| CC : | 001E01F01; 222A01 |
| FD : | Rifting; Volcanisme; Fossé; Haute résolution; Seabeam; Collection; Submersible; Modèle; Magmatisme; Subduction; Plaque Australienne; Limite plaque; Foyer; Mont sous marin; Graben; Profondeur; Ecoulement; Croûte terrestre; Basalte olivine; Andésite basaltique; Morphologie; Bilan masse; Epaisseur; Atténuation; Accrétion; Bassin Lau |
| FG : | Basalte; Roche volcanique; Roche ignée; Andésite; Océan Pacifique |
| ED : | rifting; volcanism; troughs; high resolution; Seabeam; collections; submersibles; models; magmatism; subduction; Australian Plate; plate boundaries; focus; seamounts; grabens; depth; flow; crust; olivine basalt; basaltic andesite; morphology; mass balance; thickness; attenuation; accretion; Lau Basin |
| EG : | basalts; volcanic rocks; igneous rocks; andesites; Pacific Ocean |
| SD : | Alta resolucion; Colección; Sumergible; Modelo; Magmatismo; Subducción; Límite placa; Graben; Profundidad; Corteza terrestre; Morfología; Balance masa; Espesor; Atenuación; Acreción; Cuenca Lau |
| LO : | INIST-17236.354000181715620040 |
| ID : | 10-0252673 |
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Pascal:10-0252673Le document en format XML
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Leybourne</name><affiliation><inist:fA14 i1="04"><s1>Ocean Exploration, GNS Science</s1><s2>30-368, Lower Hutt</s2><s3>NZL</s3><sZ>4 aut.</sZ></inist:fA14></affiliation></author><author><name sortKey="Hergt, J M" sort="Hergt, J M" uniqKey="Hergt J" first="J. M." last="Hergt">J. M. Hergt</name><affiliation><inist:fA14 i1="05"><s1>School of Earth Sciences, The University of Melbourne</s1><s2>VIC 3010</s2><s3>AUS</s3><sZ>5 aut.</sZ></inist:fA14></affiliation></author><author><name sortKey="Adam, C" sort="Adam, C" uniqKey="Adam C" first="C." last="Adam">C. Adam</name><affiliation><inist:fA14 i1="01"><s1>Japan Agency for Marine Earth Science and Technology</s1><s2>Yokosuka, 237-0061</s2><s3>JPN</s3><sZ>1 aut.</sZ><sZ>6 aut.</sZ></inist:fA14></affiliation></author><author><name sortKey="Mackay, K" sort="Mackay, K" uniqKey="Mackay K" first="K." last="Mackay">K. Mackay</name><affiliation><inist:fA14 i1="06"><s1>National Institute of Water and Atmospheric Research</s1><s2>14-901, Wellington</s2><s3>NZL</s3><sZ>7 aut.</sZ></inist:fA14></affiliation></author></analytic><series><title level="j" type="main">Journal of volcanology and geothermal research</title><title level="j" type="abbreviated">J. volcanol. geotherm. res.</title><idno type="ISSN">0377-0273</idno><imprint><date when="2010">2010</date></imprint></series></biblStruct></sourceDesc><seriesStmt><title level="j" type="main">Journal of volcanology and geothermal research</title><title level="j" type="abbreviated">J. volcanol. geotherm. res.</title><idno type="ISSN">0377-0273</idno></seriesStmt></fileDesc><profileDesc><textClass><keywords scheme="KwdEn" xml:lang="en"><term>Australian Plate</term><term>Lau Basin</term><term>Seabeam</term><term>accretion</term><term>attenuation</term><term>basaltic andesite</term><term>collections</term><term>crust</term><term>depth</term><term>flow</term><term>focus</term><term>grabens</term><term>high resolution</term><term>magmatism</term><term>mass balance</term><term>models</term><term>morphology</term><term>olivine basalt</term><term>plate boundaries</term><term>rifting</term><term>seamounts</term><term>subduction</term><term>submersibles</term><term>thickness</term><term>troughs</term><term>volcanism</term></keywords><keywords scheme="Pascal" xml:lang="fr"><term>Rifting</term><term>Volcanisme</term><term>Fossé</term><term>Haute résolution</term><term>Seabeam</term><term>Collection</term><term>Submersible</term><term>Modèle</term><term>Magmatisme</term><term>Subduction</term><term>Plaque Australienne</term><term>Limite plaque</term><term>Foyer</term><term>Mont sous marin</term><term>Graben</term><term>Profondeur</term><term>Ecoulement</term><term>Croûte terrestre</term><term>Basalte olivine</term><term>Andésite basaltique</term><term>Morphologie</term><term>Bilan masse</term><term>Epaisseur</term><term>Atténuation</term><term>Accrétion</term><term>Bassin Lau</term></keywords></textClass></profileDesc></teiHeader><front><div type="abstract" xml:lang="en">High resolution multibeam (EM300 and SEABEAM) data of the Southern Havre Trough (SHT), combined with observations and sample collections from the submersible Shinkai6500 and deep-tow camera, are used to develop a model for the evolution and magmatism of this backarc system. The Havre Trough and the associated Kermadec Arc are the product of westward subduction at the Pacific-Australian plate boundary. Detailed studies focus on newly discovered features including a seamount (Saito Seamount) and a deep graben (Ngatoroirangi Rift, >4000 m water depth floored with a constructional axial volcanic ridge > 5 km in length and in excess of 200 m high), both of which are characterised by pillow and lobate flows estimated at <20,000 years old based on sediment cover, high reflectivity and thin Mn crusts on recovered glassy olivine basalts and basaltic andesites. Elongate volcanic ridges at 35°15'S and 34°30'S, and backarc seamounts (35°30'S,178°30'E) occur at the eastern margin of the SHT. Similar seafloor morphology is observed in the central and western portions of the basin, suggesting that recent volcanism may be broadly distributed across the backarc. Mass balance modelling indicates a maximum crustal thickness of ˜11 km to <6 krn, similar to estimates of crustal thickness in the Lau Basin to the north. Given such high crustal attenuation and extensive backarc mafic magmatism within deep SHT rifts, we propose that the SHT is in an incipient phase of distributed and "disorganised" oceanic crustal accretion in multiple, ephemeral, and short but deep (>4000 m) spreading systems. These discontinuous spreading systems are characterised by failed rifts, rift segmentation, and propagation. Successive episodes of magmatic intrusion into thinned faulted arc basement results in defocused asymmetrical accretion. Cross-arc volcanic chains, isolated volcanoes and underlying basement plateaus are interpreted to represent a "cap" of recent extrusives. However, they may also be composed entirely of newly accreted crust and the spatially extensive basement fabric of elongated volcanic ridges may be the surface expression of pervasive dike intrusion that has thoroughly penetrated and essentially replaced the original arc crust with newly accreted intrusives.</div></front></TEI><inist><standard h6="B"><pA><fA01 i1="01" i2="1"><s0>0377-0273</s0></fA01><fA02 i1="01"><s0>JVGRDQ</s0></fA02><fA03 i2="1"><s0>J. volcanol. geotherm. res.</s0></fA03><fA05><s2>190</s2></fA05><fA06><s2>1-2</s2></fA06><fA08 i1="01" i2="1" l="ENG"><s1>Backarc rifting, constructional volcanism and nascent disorganised spreading in the southern Havre Trough backarc rifts (SW Pacific)</s1></fA08><fA09 i1="01" i2="1" l="ENG"><s1>Making and Breaking the Arc: A Volume in Honour of Professor John Gamble</s1></fA09><fA11 i1="01" i2="1"><s1>WYSOCZANSKI (Rj.)</s1></fA11><fA11 i1="02" i2="1"><s1>TODD (E.)</s1></fA11><fA11 i1="03" i2="1"><s1>WRIGHT (I. C.)</s1></fA11><fA11 i1="04" i2="1"><s1>LEYBOURNE (M. I.)</s1></fA11><fA11 i1="05" i2="1"><s1>HERGT (J. M.)</s1></fA11><fA11 i1="06" i2="1"><s1>ADAM (C.)</s1></fA11><fA11 i1="07" i2="1"><s1>MACKAY (K.)</s1></fA11><fA12 i1="01" i2="1"><s1>WYSOCZANSKI (Richard J.)</s1><s9>ed.</s9></fA12><fA12 i1="02" i2="1"><s1>ROWLAND (Julie V.)</s1><s9>ed.</s9></fA12><fA12 i1="03" i2="1"><s1>BEKER (Joel A.)</s1><s9>ed.</s9></fA12><fA12 i1="04" i2="1"><s1>WILSON (Colin J. N.)</s1><s9>ed.</s9></fA12><fA14 i1="01"><s1>Japan Agency for Marine Earth Science and Technology</s1><s2>Yokosuka, 237-0061</s2><s3>JPN</s3><sZ>1 aut.</sZ><sZ>6 aut.</sZ></fA14><fA14 i1="02"><s1>Department of Earth and Planetary Sciences, University of California, Santa Cruz, 1156 High St.</s1><s2>Santa Cruz, CA, 95064</s2><s3>USA</s3><sZ>2 aut.</sZ></fA14><fA14 i1="03"><s1>National Oceanography Centre, Southampton, Empress Dock</s1><s2>European Way, Southampton SO14 3ZH</s2><s3>GBR</s3><sZ>3 aut.</sZ></fA14><fA14 i1="04"><s1>Ocean Exploration, GNS Science</s1><s2>30-368, Lower Hutt</s2><s3>NZL</s3><sZ>4 aut.</sZ></fA14><fA14 i1="05"><s1>School of Earth Sciences, The University of Melbourne</s1><s2>VIC 3010</s2><s3>AUS</s3><sZ>5 aut.</sZ></fA14><fA14 i1="06"><s1>National Institute of Water and Atmospheric Research</s1><s2>14-901, Wellington</s2><s3>NZL</s3><sZ>7 aut.</sZ></fA14><fA15 i1="01"><s1>National Institute of Water and Atmospheric Research, Private Bag 14901</s1><s2>Wellington 6041</s2><s3>NZL</s3><sZ>1 aut.</sZ></fA15><fA15 i1="02"><s1>School of Geography, Environment and Earth Sciences, Victoria University of Wellington, PO Box 600</s1><s2>Wellington 6041</s2><s3>NZL</s3><sZ>1 aut.</sZ><sZ>3 aut.</sZ><sZ>4 aut.</sZ></fA15><fA15 i1="03"><s1>School of Environment, University of Auckland, Private Bag 92019</s1><s2>Auckland 1142</s2><s3>NZL</s3><sZ>2 aut.</sZ></fA15><fA20><s1>39-57</s1></fA20><fA21><s1>2010</s1></fA21><fA23 i1="01"><s0>ENG</s0></fA23><fA43 i1="01"><s1>INIST</s1><s2>17236</s2><s5>354000181715620040</s5></fA43><fA44><s0>0000</s0><s1>© 2010 INIST-CNRS. All rights reserved.</s1></fA44><fA45><s0>1 p.1/2</s0></fA45><fA47 i1="01" i2="1"><s0>10-0252673</s0></fA47><fA60><s1>P</s1></fA60><fA61><s0>A</s0></fA61><fA64 i1="01" i2="1"><s0>Journal of volcanology and geothermal research</s0></fA64><fA66 i1="01"><s0>GBR</s0></fA66><fC01 i1="01" l="ENG"><s0>High resolution multibeam (EM300 and SEABEAM) data of the Southern Havre Trough (SHT), combined with observations and sample collections from the submersible Shinkai6500 and deep-tow camera, are used to develop a model for the evolution and magmatism of this backarc system. The Havre Trough and the associated Kermadec Arc are the product of westward subduction at the Pacific-Australian plate boundary. Detailed studies focus on newly discovered features including a seamount (Saito Seamount) and a deep graben (Ngatoroirangi Rift, >4000 m water depth floored with a constructional axial volcanic ridge > 5 km in length and in excess of 200 m high), both of which are characterised by pillow and lobate flows estimated at <20,000 years old based on sediment cover, high reflectivity and thin Mn crusts on recovered glassy olivine basalts and basaltic andesites. Elongate volcanic ridges at 35°15'S and 34°30'S, and backarc seamounts (35°30'S,178°30'E) occur at the eastern margin of the SHT. Similar seafloor morphology is observed in the central and western portions of the basin, suggesting that recent volcanism may be broadly distributed across the backarc. Mass balance modelling indicates a maximum crustal thickness of ˜11 km to <6 krn, similar to estimates of crustal thickness in the Lau Basin to the north. Given such high crustal attenuation and extensive backarc mafic magmatism within deep SHT rifts, we propose that the SHT is in an incipient phase of distributed and "disorganised" oceanic crustal accretion in multiple, ephemeral, and short but deep (>4000 m) spreading systems. These discontinuous spreading systems are characterised by failed rifts, rift segmentation, and propagation. Successive episodes of magmatic intrusion into thinned faulted arc basement results in defocused asymmetrical accretion. Cross-arc volcanic chains, isolated volcanoes and underlying basement plateaus are interpreted to represent a "cap" of recent extrusives. However, they may also be composed entirely of newly accreted crust and the spatially extensive basement fabric of elongated volcanic ridges may be the surface expression of pervasive dike intrusion that has thoroughly penetrated and essentially replaced the original arc crust with newly accreted intrusives.</s0></fC01><fC02 i1="01" i2="2"><s0>001E01F01</s0></fC02><fC02 i1="02" i2="2"><s0>222A01</s0></fC02><fC03 i1="01" i2="2" l="FRE"><s0>Rifting</s0><s5>01</s5></fC03><fC03 i1="01" i2="2" l="ENG"><s0>rifting</s0><s5>01</s5></fC03><fC03 i1="02" i2="2" l="FRE"><s0>Volcanisme</s0><s5>02</s5></fC03><fC03 i1="02" i2="2" l="ENG"><s0>volcanism</s0><s5>02</s5></fC03><fC03 i1="03" i2="2" l="FRE"><s0>Fossé</s0><s5>03</s5></fC03><fC03 i1="03" i2="2" l="ENG"><s0>troughs</s0><s5>03</s5></fC03><fC03 i1="04" i2="2" l="FRE"><s0>Haute résolution</s0><s5>04</s5></fC03><fC03 i1="04" i2="2" l="ENG"><s0>high resolution</s0><s5>04</s5></fC03><fC03 i1="04" i2="2" l="SPA"><s0>Alta resolucion</s0><s5>04</s5></fC03><fC03 i1="05" i2="2" l="FRE"><s0>Seabeam</s0><s5>05</s5></fC03><fC03 i1="05" i2="2" l="ENG"><s0>Seabeam</s0><s5>05</s5></fC03><fC03 i1="06" i2="2" l="FRE"><s0>Collection</s0><s5>06</s5></fC03><fC03 i1="06" i2="2" l="ENG"><s0>collections</s0><s5>06</s5></fC03><fC03 i1="06" i2="2" l="SPA"><s0>Colección</s0><s5>06</s5></fC03><fC03 i1="07" i2="2" l="FRE"><s0>Submersible</s0><s5>07</s5></fC03><fC03 i1="07" i2="2" l="ENG"><s0>submersibles</s0><s5>07</s5></fC03><fC03 i1="07" i2="2" l="SPA"><s0>Sumergible</s0><s5>07</s5></fC03><fC03 i1="08" i2="2" l="FRE"><s0>Modèle</s0><s5>08</s5></fC03><fC03 i1="08" i2="2" l="ENG"><s0>models</s0><s5>08</s5></fC03><fC03 i1="08" i2="2" l="SPA"><s0>Modelo</s0><s5>08</s5></fC03><fC03 i1="09" i2="2" l="FRE"><s0>Magmatisme</s0><s5>09</s5></fC03><fC03 i1="09" i2="2" l="ENG"><s0>magmatism</s0><s5>09</s5></fC03><fC03 i1="09" i2="2" l="SPA"><s0>Magmatismo</s0><s5>09</s5></fC03><fC03 i1="10" i2="2" l="FRE"><s0>Subduction</s0><s5>10</s5></fC03><fC03 i1="10" i2="2" l="ENG"><s0>subduction</s0><s5>10</s5></fC03><fC03 i1="10" i2="2" l="SPA"><s0>Subducción</s0><s5>10</s5></fC03><fC03 i1="11" i2="2" l="FRE"><s0>Plaque Australienne</s0><s5>11</s5></fC03><fC03 i1="11" i2="2" l="ENG"><s0>Australian Plate</s0><s5>11</s5></fC03><fC03 i1="12" i2="2" l="FRE"><s0>Limite plaque</s0><s5>12</s5></fC03><fC03 i1="12" i2="2" l="ENG"><s0>plate boundaries</s0><s5>12</s5></fC03><fC03 i1="12" i2="2" l="SPA"><s0>Límite placa</s0><s5>12</s5></fC03><fC03 i1="13" i2="2" l="FRE"><s0>Foyer</s0><s5>13</s5></fC03><fC03 i1="13" i2="2" l="ENG"><s0>focus</s0><s5>13</s5></fC03><fC03 i1="14" i2="2" l="FRE"><s0>Mont sous marin</s0><s5>14</s5></fC03><fC03 i1="14" i2="2" l="ENG"><s0>seamounts</s0><s5>14</s5></fC03><fC03 i1="15" i2="2" l="FRE"><s0>Graben</s0><s5>15</s5></fC03><fC03 i1="15" i2="2" l="ENG"><s0>grabens</s0><s5>15</s5></fC03><fC03 i1="15" i2="2" l="SPA"><s0>Graben</s0><s5>15</s5></fC03><fC03 i1="16" i2="2" l="FRE"><s0>Profondeur</s0><s5>16</s5></fC03><fC03 i1="16" i2="2" l="ENG"><s0>depth</s0><s5>16</s5></fC03><fC03 i1="16" i2="2" l="SPA"><s0>Profundidad</s0><s5>16</s5></fC03><fC03 i1="17" i2="2" l="FRE"><s0>Ecoulement</s0><s5>17</s5></fC03><fC03 i1="17" i2="2" l="ENG"><s0>flow</s0><s5>17</s5></fC03><fC03 i1="18" i2="2" l="FRE"><s0>Croûte terrestre</s0><s5>18</s5></fC03><fC03 i1="18" i2="2" l="ENG"><s0>crust</s0><s5>18</s5></fC03><fC03 i1="18" i2="2" l="SPA"><s0>Corteza terrestre</s0><s5>18</s5></fC03><fC03 i1="19" i2="2" l="FRE"><s0>Basalte olivine</s0><s2>NV</s2><s5>19</s5></fC03><fC03 i1="19" i2="2" l="ENG"><s0>olivine basalt</s0><s2>NV</s2><s5>19</s5></fC03><fC03 i1="20" i2="2" l="FRE"><s0>Andésite basaltique</s0><s2>NV</s2><s5>20</s5></fC03><fC03 i1="20" i2="2" l="ENG"><s0>basaltic andesite</s0><s2>NV</s2><s5>20</s5></fC03><fC03 i1="21" i2="2" l="FRE"><s0>Morphologie</s0><s5>21</s5></fC03><fC03 i1="21" i2="2" l="ENG"><s0>morphology</s0><s5>21</s5></fC03><fC03 i1="21" i2="2" l="SPA"><s0>Morfología</s0><s5>21</s5></fC03><fC03 i1="22" i2="2" l="FRE"><s0>Bilan masse</s0><s5>22</s5></fC03><fC03 i1="22" i2="2" l="ENG"><s0>mass balance</s0><s5>22</s5></fC03><fC03 i1="22" i2="2" l="SPA"><s0>Balance masa</s0><s5>22</s5></fC03><fC03 i1="23" i2="2" l="FRE"><s0>Epaisseur</s0><s5>23</s5></fC03><fC03 i1="23" i2="2" l="ENG"><s0>thickness</s0><s5>23</s5></fC03><fC03 i1="23" i2="2" l="SPA"><s0>Espesor</s0><s5>23</s5></fC03><fC03 i1="24" i2="2" l="FRE"><s0>Atténuation</s0><s5>24</s5></fC03><fC03 i1="24" i2="2" l="ENG"><s0>attenuation</s0><s5>24</s5></fC03><fC03 i1="24" i2="2" l="SPA"><s0>Atenuación</s0><s5>24</s5></fC03><fC03 i1="25" i2="2" l="FRE"><s0>Accrétion</s0><s5>25</s5></fC03><fC03 i1="25" i2="2" l="ENG"><s0>accretion</s0><s5>25</s5></fC03><fC03 i1="25" i2="2" l="SPA"><s0>Acreción</s0><s5>25</s5></fC03><fC03 i1="26" i2="2" l="FRE"><s0>Bassin Lau</s0><s2>NG</s2><s5>61</s5></fC03><fC03 i1="26" i2="2" l="ENG"><s0>Lau Basin</s0><s2>NG</s2><s5>61</s5></fC03><fC03 i1="26" i2="2" l="SPA"><s0>Cuenca Lau</s0><s2>NG</s2><s5>61</s5></fC03><fC07 i1="01" i2="2" l="FRE"><s0>Basalte</s0><s2>NV</s2></fC07><fC07 i1="01" i2="2" l="ENG"><s0>basalts</s0><s2>NV</s2></fC07><fC07 i1="01" i2="2" l="SPA"><s0>Basalto</s0><s2>NV</s2></fC07><fC07 i1="02" i2="2" l="FRE"><s0>Roche volcanique</s0><s2>NV</s2></fC07><fC07 i1="02" i2="2" l="ENG"><s0>volcanic rocks</s0><s2>NV</s2></fC07><fC07 i1="02" i2="2" l="SPA"><s0>Roca volcánica</s0><s2>NV</s2></fC07><fC07 i1="03" i2="2" l="FRE"><s0>Roche ignée</s0><s2>NV</s2></fC07><fC07 i1="03" i2="2" l="ENG"><s0>igneous rocks</s0><s2>NV</s2></fC07><fC07 i1="03" i2="2" l="SPA"><s0>Roca ignea</s0><s2>NV</s2></fC07><fC07 i1="04" i2="2" l="FRE"><s0>Andésite</s0><s2>NV</s2></fC07><fC07 i1="04" i2="2" l="ENG"><s0>andesites</s0><s2>NV</s2></fC07><fC07 i1="04" i2="2" l="SPA"><s0>Andesita</s0><s2>NV</s2></fC07><fC07 i1="05" i2="2" l="FRE"><s0>Océan Pacifique</s0><s2>564</s2></fC07><fC07 i1="05" i2="2" l="ENG"><s0>Pacific Ocean</s0><s2>564</s2></fC07><fC07 i1="05" i2="2" l="SPA"><s0>Océano Pacífico</s0><s2>564</s2></fC07><fN21><s1>165</s1></fN21><fN44 i1="01"><s1>OTO</s1></fN44><fN82><s1>OTO</s1></fN82></pA></standard><server><NO>PASCAL 10-0252673 INIST</NO><ET>Backarc rifting, constructional volcanism and nascent disorganised spreading in the southern Havre Trough backarc rifts (SW Pacific)</ET><AU>WYSOCZANSKI (Rj.); TODD (E.); WRIGHT (I. C.); LEYBOURNE (M. I.); HERGT (J. M.); ADAM (C.); MACKAY (K.); WYSOCZANSKI (Richard J.); ROWLAND (Julie V.); BEKER (Joel A.); WILSON (Colin J. N.)</AU><AF>Japan Agency for Marine Earth Science and Technology/Yokosuka, 237-0061/Japon (1 aut., 6 aut.); Department of Earth and Planetary Sciences, University of California, Santa Cruz, 1156 High St./Santa Cruz, CA, 95064/Etats-Unis (2 aut.); National Oceanography Centre, Southampton, Empress Dock/European Way, Southampton SO14 3ZH/Royaume-Uni (3 aut.); Ocean Exploration, GNS Science/30-368, Lower Hutt/Nouvelle-Zélande (4 aut.); School of Earth Sciences, The University of Melbourne/VIC 3010/Australie (5 aut.); National Institute of Water and Atmospheric Research/14-901, Wellington/Nouvelle-Zélande (7 aut.); National Institute of Water and Atmospheric Research, Private Bag 14901/Wellington 6041/Nouvelle-Zélande (1 aut.); School of Geography, Environment and Earth Sciences, Victoria University of Wellington, PO Box 600/Wellington 6041/Nouvelle-Zélande (1 aut., 3 aut., 4 aut.); School of Environment, University of Auckland, Private Bag 92019/Auckland 1142/Nouvelle-Zélande (2 aut.)</AF><DT>Publication en série; Niveau analytique</DT><SO>Journal of volcanology and geothermal research; ISSN 0377-0273; Coden JVGRDQ; Royaume-Uni; Da. 2010; Vol. 190; No. 1-2; Pp. 39-57; Bibl. 1 p.1/2</SO><LA>Anglais</LA><EA>High resolution multibeam (EM300 and SEABEAM) data of the Southern Havre Trough (SHT), combined with observations and sample collections from the submersible Shinkai6500 and deep-tow camera, are used to develop a model for the evolution and magmatism of this backarc system. The Havre Trough and the associated Kermadec Arc are the product of westward subduction at the Pacific-Australian plate boundary. Detailed studies focus on newly discovered features including a seamount (Saito Seamount) and a deep graben (Ngatoroirangi Rift, >4000 m water depth floored with a constructional axial volcanic ridge > 5 km in length and in excess of 200 m high), both of which are characterised by pillow and lobate flows estimated at <20,000 years old based on sediment cover, high reflectivity and thin Mn crusts on recovered glassy olivine basalts and basaltic andesites. Elongate volcanic ridges at 35°15'S and 34°30'S, and backarc seamounts (35°30'S,178°30'E) occur at the eastern margin of the SHT. Similar seafloor morphology is observed in the central and western portions of the basin, suggesting that recent volcanism may be broadly distributed across the backarc. Mass balance modelling indicates a maximum crustal thickness of ˜11 km to <6 krn, similar to estimates of crustal thickness in the Lau Basin to the north. Given such high crustal attenuation and extensive backarc mafic magmatism within deep SHT rifts, we propose that the SHT is in an incipient phase of distributed and "disorganised" oceanic crustal accretion in multiple, ephemeral, and short but deep (>4000 m) spreading systems. These discontinuous spreading systems are characterised by failed rifts, rift segmentation, and propagation. Successive episodes of magmatic intrusion into thinned faulted arc basement results in defocused asymmetrical accretion. Cross-arc volcanic chains, isolated volcanoes and underlying basement plateaus are interpreted to represent a "cap" of recent extrusives. However, they may also be composed entirely of newly accreted crust and the spatially extensive basement fabric of elongated volcanic ridges may be the surface expression of pervasive dike intrusion that has thoroughly penetrated and essentially replaced the original arc crust with newly accreted intrusives.</EA><CC>001E01F01; 222A01</CC><FD>Rifting; Volcanisme; Fossé; Haute résolution; Seabeam; Collection; Submersible; Modèle; Magmatisme; Subduction; Plaque Australienne; Limite plaque; Foyer; Mont sous marin; Graben; Profondeur; Ecoulement; Croûte terrestre; Basalte olivine; Andésite basaltique; Morphologie; Bilan masse; Epaisseur; Atténuation; Accrétion; Bassin Lau</FD><FG>Basalte; Roche volcanique; Roche ignée; Andésite; Océan Pacifique</FG><ED>rifting; volcanism; troughs; high resolution; Seabeam; collections; submersibles; models; magmatism; subduction; Australian Plate; plate boundaries; focus; seamounts; grabens; depth; flow; crust; olivine basalt; basaltic andesite; morphology; mass balance; thickness; attenuation; accretion; Lau Basin</ED><EG>basalts; volcanic rocks; igneous rocks; andesites; Pacific Ocean</EG><SD>Alta resolucion; Colección; Sumergible; Modelo; Magmatismo; Subducción; Límite placa; Graben; Profundidad; Corteza terrestre; Morfología; Balance masa; Espesor; Atenuación; Acreción; Cuenca Lau</SD><LO>INIST-17236.354000181715620040</LO><ID>10-0252673</ID></server></inist></record>Pour manipuler ce document sous Unix (Dilib)
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