冲绳海槽现代张裂的地球物理特征
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摘要
位于东海陆架与琉球岛弧之间的冲绳海槽为板块俯冲作用形成的弧后断陷盆地,具有独特的构造地貌特征。自中新世末以来历经了4个强烈拉张的演化时期,目前已达到张裂的高级阶段。地球物理资料显示,海槽中的现代拉张作用仍在进行,表现在海槽轴部快速沉降形成地堑槽,对称分布的张性断裂,晚更新世—全新世以来的岩浆活动,从老至新排列的磁异常条带以及高地热流、频繁的地震活动等,充分体现了冲绳海槽的现代扩张特点。
Okinawa Trough,a back-arc fault basin that was formed by the plate collision and subduction,is located between the continental shelf of the East China Sea and Ryukyu Island arc.It has unique tectonic geomorphological features.The back-arc faulting started in Miocene,and the tension of fracture is continuing now.Okinawa Trough has undergone four intensive stages of tension evolution since the end of Miocene and now it is in the high stage of tension.According to geophysical data,modern tension action is still active in the Trough.For examples,the graben trough was caused by rapid subsidence of the axis of the Okinawa Trough and tension faults were formed symmetrically,and aslo there were magmatic activities,frequent earthquakes and high heat-flow phenomena from late Pleistocene to Holocene In addition,there are the zones of magnetic anomalies ranging from old to new ones.The tension characteristics of the Okinawa Trough in modern times have sufficiently been proved.
Okinawa Trough,a back-arc fault basin that was formed by the plate collision and subduction,is located between the continental shelf of the East China Sea and Ryukyu Island arc.It has unique tectonic geomorphological features.The back-arc faulting started in Miocene,and the tension of fracture is continuing now.Okinawa Trough has undergone four intensive stages of tension evolution since the end of Miocene and now it is in the high stage of tension.According to geophysical data,modern tension action is still active in the Trough.For examples,the graben trough was caused by rapid subsidence of the axis of the Okinawa Trough and tension faults were formed symmetrically,and aslo there were magmatic activities,frequent earthquakes and high heat-flow phenomena from late Pleistocene to Holocene In addition,there are the zones of magnetic anomalies ranging from old to new ones.The tension characteristics of the Okinawa Trough in modern times have sufficiently been proved.
引文
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[5] 梁瑞才,吴金龙,刘保华,等.冲绳海槽中段线性磁异常条带及其构造发育[J\〗.海洋学报,2001,23(2).[LIANGRui cai,WUJin long,LIUBao hua,etal.LinearmagneticanomaliesandtectonicdevelopmentforthemiddleOkinawaTrough[J].ActaOceanologicaSinica,2001,23(2).]
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[7] Couiallo.冲绳海槽盆地张开和台湾碰撞[J].海洋地质译丛,1987.[Couiallo.BasinopeningofOkinawaTroughandcomingintocollisionwithTaiwan[J].Translationcollectionmarinegeology,1987.]
[8] 渡边,LangsethMG.西太平洋弧后盆地的热流[A].东海地质译文集汇编[C].1980.89—115.[渡边,langsethMG.Geothermalheatflowinback arcbasinofthewestPacific[A].CollectionofgeologicalversionofEastChinaSea(4)[C\〗.1980.89—115.]
[9] 周祖翼,廖宗廷,金性春,等.冲绳海槽———弧后背景下大陆张裂的最高阶段[J].海洋地质与第四纪地质,2001,21(1):51—55.[ZHOUZu yi,LIAOZong ting,JINXing chun,etal.OkinawaTrough:Thehigheststageofcontinentaltensionriftinginback arcsetting[J].MarineGeologyandQuaternaryGeology,2001,21(1):51—55.]
[10] MurphyRW.马尼拉海沟-台湾西部褶皱带:一条反转的俯冲带[A].东海地质译文汇编[C].1980.201—214.[MurphyRW.OceanictrenchofManila FoldbelttothewestofTaiwan:Areversedsubductionbelt[A].CollectionofgeologicalversionofEastChinaSea(4)[C].1980.201—214.]
[2] 木村政昭著,沈耀龙译.冲绳海槽地堑的形成[A].琉球群岛、冲绳海槽、钓鱼岛地质[C].1987.23—48.[木村政昭,SHENYaolong.ThegrabenformationintheOkinawaTrough[A].GeologyofRyukyuArchipelago,OkinawaTroughandDiaoyuIsland[C].1987.23—48.]
[3] MauriceJT.亚洲东部新生代构造运动[A].东海地质译文汇编(四)[C].1980.56—58.[MauriceJT.CenozoicEratectogenesisofEastAsia[A].CollectionofgeologicalversionofEastChinaSea(4)[C].1980.56—58.]
[4] 李昭兴,ShorG.冲绳海槽:一个弧后盆地的成因[A].东海地质译文汇编[C].1980.147—162.[LIZhao xing,ShorG.OkinawaTrough:Anoriginofaback arcbasin[A].CollectionofgeologicalversionofEastChinaSea(4)[C].1980.147-162]
[5] 梁瑞才,吴金龙,刘保华,等.冲绳海槽中段线性磁异常条带及其构造发育[J\〗.海洋学报,2001,23(2).[LIANGRui cai,WUJin long,LIUBao hua,etal.LinearmagneticanomaliesandtectonicdevelopmentforthemiddleOkinawaTrough[J].ActaOceanologicaSinica,2001,23(2).]
[6] 业治铮,张明书.冲绳海槽晚更新世—全新世沉积物的初步研究[J].海洋地质与第四纪地质,1983,3(2):1—26.[YEZhizheng,ZHANGMing shu.PreliminarystudyonthelatePleistoceneandHolocenesedimentsamplesfromOkinawaTrough[J].MarineGeologyandQuaternaryGeology,1983,3(2):1—26.]
[7] Couiallo.冲绳海槽盆地张开和台湾碰撞[J].海洋地质译丛,1987.[Couiallo.BasinopeningofOkinawaTroughandcomingintocollisionwithTaiwan[J].Translationcollectionmarinegeology,1987.]
[8] 渡边,LangsethMG.西太平洋弧后盆地的热流[A].东海地质译文集汇编[C].1980.89—115.[渡边,langsethMG.Geothermalheatflowinback arcbasinofthewestPacific[A].CollectionofgeologicalversionofEastChinaSea(4)[C\〗.1980.89—115.]
[9] 周祖翼,廖宗廷,金性春,等.冲绳海槽———弧后背景下大陆张裂的最高阶段[J].海洋地质与第四纪地质,2001,21(1):51—55.[ZHOUZu yi,LIAOZong ting,JINXing chun,etal.OkinawaTrough:Thehigheststageofcontinentaltensionriftinginback arcsetting[J].MarineGeologyandQuaternaryGeology,2001,21(1):51—55.]
[10] MurphyRW.马尼拉海沟-台湾西部褶皱带:一条反转的俯冲带[A].东海地质译文汇编[C].1980.201—214.[MurphyRW.OceanictrenchofManila FoldbelttothewestofTaiwan:Areversedsubductionbelt[A].CollectionofgeologicalversionofEastChinaSea(4)[C].1980.201—214.]
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