卡罗琳海板块实验:初始俯冲、初始扩张与流固耦合

李春峰, 李刚, 厉子龙, 刘文潇, 章露露, 陆哲哲, 陈雪刚, 姚泽伟

李春峰, 李刚, 厉子龙, 刘文潇, 章露露, 陆哲哲, 陈雪刚, 姚泽伟. 卡罗琳海板块实验:初始俯冲、初始扩张与流固耦合[J]. 海洋地质与第四纪地质, 2019, 39(5): 87-97. DOI: 10.16562/j.cnki.0256-1492.2019031501
引用本文: 李春峰, 李刚, 厉子龙, 刘文潇, 章露露, 陆哲哲, 陈雪刚, 姚泽伟. 卡罗琳海板块实验:初始俯冲、初始扩张与流固耦合[J]. 海洋地质与第四纪地质, 2019, 39(5): 87-97. DOI: 10.16562/j.cnki.0256-1492.2019031501
LI Chunfeng, LI Gang, LI Zilong, LIU Wenxiao, ZHANG Lulu, LU Zhezhe, CHEN Xuegang, YAO Zewei. Study of the Caroline plate: Initial subduction, initial spreading and fluid-solid interaction[J]. Marine Geology & Quaternary Geology, 2019, 39(5): 87-97. DOI: 10.16562/j.cnki.0256-1492.2019031501
Citation: LI Chunfeng, LI Gang, LI Zilong, LIU Wenxiao, ZHANG Lulu, LU Zhezhe, CHEN Xuegang, YAO Zewei. Study of the Caroline plate: Initial subduction, initial spreading and fluid-solid interaction[J]. Marine Geology & Quaternary Geology, 2019, 39(5): 87-97. DOI: 10.16562/j.cnki.0256-1492.2019031501

卡罗琳海板块实验:初始俯冲、初始扩张与流固耦合

基金项目: 国家自然科学基金重大研究计划重点项目“西太平洋地球系统多圈层相互作用”(91858213);国家自然科学基金面上项目“太平洋岩石圈热演化研究”(41776057)
详细信息
    作者简介:

    李春峰(1970—),男,教授,主要从事应用地球物理与地球动力学研究,E-mail:cfli@zju.edu.cn

  • 中图分类号: P738.1

Study of the Caroline plate: Initial subduction, initial spreading and fluid-solid interaction

  • 摘要: 西太平洋具有全球最活跃的板块构造与海陆相互作用过程,西太平洋的卡罗琳(Caroline)海盆形成于特提斯海与太平洋之间,处于印尼海道的咽喉区域,海盆范围正好对应了西太平洋暖池的大部分海域。其内部地形复杂,具有特征的隆起和残留洋中脊,而周围具有年轻活跃的俯冲带和洋中脊,并且与菲律宾海、太平洋、Ontong-Java大火成岩省、众多深海沟等相互作用,是研究俯冲带和洋中脊初始形成机理与动力学以及固体地球与海水相互作用的理想场所。过去对Caroline海盆的研究主要是美国和日本科学家在20世纪70—80年代完成的,在很多构造单元的成因和属性的解释上存在很大争议,很少涉及多圈层相互作用方面的研究。国家自然科学基金委重大研究计划“西太平洋地球系统多圈层相互作用”的实施推动了西太平洋基础海洋科学研究的步伐,通过综合地球物理和地球化学分析,对Caroline海盆的构造边界过程和海盆岩石圈蛇纹岩化程度等开展详细研究,探索深部过程与海底过程之间,特别是在水和热流通量方面的联系。Caroline海盆是提出典型海洋微板块演化模式和未来进一步深入研究(包括科学大洋钻探)的关键区域,其复杂多样的边界发育初始俯冲边界、初始扩张边界以及火山链和张裂中心,其板内地质构造也曾存在复杂的海底扩张和构造转换,并且显示强烈的板块边界和板内构造耦合过程。
    Abstract: The western Pacific has the most active plate tectonic processes and land-ocean interactions. The Caroline Basin is a small plate formed between the Tethys and the Pacific, currently located at the throat of the Indonesian seaway, and takes a large area of the western Pacific warm pool. The Caroline plate is rather complex topographically and is characterized by ridges and relic spreading centers. The plate is bordered by young active subduction zones and active spreading centers, and strongly interacts with the surrounding Philippine Sea plate, the Pacific plate, the Ontong-Java large igneous province, and many deep trenches. Therefore, it is an ideal place for studying process and dynamics of initiation of subduction and seafloor spreading, as well as the interaction of the solid earth with seawater. In the past, the investigation of the Caroline Basin was done mostly in the 70—80 s of last century. So far, many controversies remain unsolved on the nature and genesis of some tectonic units, and the interactions among multiple geospheres were seldom explored. The implementation of the major research project on " Multi-sphere Interaction of the Western Pacific Earth System” supported by the National Natural Science Foundation of China greatly accelerate the pace of marine research in the Western Pacific region. In this project, we conduct comprehensive geophysical and geochemical analyses of the tectonic boundary process of the Caroline Basin and the extent of serpentinization of the uppermost lithospheric mantle in the basin. We also examine the coupling between the deep process in the lithosphere and the shallow process on the seabed, in particular the relationship between water and heat flux. Based upon the research, we propose in this paper an evolutional model for this unique oceanic micro-plate and its tectonic boundaries. Further research activities, including scientific ocean drilling, are recommended.
  • 中生代-新生代之交,西太平洋地区发生了大的构造板块调整,比如印度板块向欧亚板块的楔入、太平洋板块向东后撤以及太平洋板块运动方向由北北西向转变为北西西向(50 Ma左右)等,这些综合效应导致了西太平洋区域形成了巨大的沟-弧-盆体系[1-5]。菲律宾海板块是西太平洋地区在此期间形成的最大的边缘海之一(图1),其形成和演化对其邻近区域的岩浆活动和构造演化产生了深远的影响。过去的几十年里,以大洋钻探计划为首的众多航次(包括DSDP (深海钻探计划)6、31、58、59、60, ODP (大洋钻探计划)195, IODP (综合大洋钻探计划)331, IODP (大洋发现计划) 350—352航次)对菲律宾海板块开展了详细的钻探取样工作,获得了大量的底质(沉积物和岩石)样品和地质地球物理资料,取得了一系列重要的研究成果[6-11]。但仍有一些关键的科学问题亟待解决,比如,(1)俯冲是如何启动的[12]?科学家提出了2种俯冲初始的模型,一种是由于相邻板块的密度差引起的自发过程,另一种观点认为俯冲初始是邻近板块的横向驱动力所导致的一个诱发过程[12]。(2)弧后盆地的成因机制?对于西菲律宾海盆的成因目前共有3种模型,包括弧后扩张成因、捕获的洋壳片段成因以及弧后扩张和地幔柱共同作用成因[10, 13-15]。(3)菲律宾海板内岩浆作用的动力学机制?目前存在两种认识,一种是过量残余岩浆成因,另一种是地幔柱成因[10, 14-16]。(4)俯冲过程中的物质循环[11]

    图  1  菲律宾海板块及主要构造单元
    Figure  1.  Philippine Sea plate and the main tectonic units

    菲律宾海板块由一系列的弧后盆地和残余弧脊及活动岛弧组成,自西向东分别为西菲律宾海盆、四国海盆、帕里西维拉海盆和马里亚纳海槽以及九州-帕劳脊、西马里亚纳脊和伊豆-小笠原-马里亚纳(IBM)弧。其中的帕里西维拉海盆与其北侧的四国海盆以及南海和日本海等均为西太平洋第二扩张幕形成的弧后盆地。DSDP 6和DSDP 59等航次对帕里西维拉海盆开展了详细的调查,取得了一系列重要的认识[11, 17]。研究表明,帕里西维拉海盆在地形上具有东西不对称的特征,其基底熔岩具有类似于弧后盆地玄武岩(BABB)的微量元素特点和印度洋型MORB的同位素特征[6, 18]。然而,帕里西维拉海盆还存在一系列的科学问题亟待解决,比如,帕里西维拉扩张动力学过程、深部地幔源区性质,扩张后海山及核杂岩成因机制,以及该海盆的沉积过程与古海洋古气候演化等,还不是很清晰。本文在总结前人对于该海盆研究成果的基础上,提出了目前尚存在的重要科学问题以及未来可能的钻探位置建议。

    菲律宾海是西太平洋最大的边缘海之一,面积约为540万km2,位于欧亚板块、印度-澳大利亚板块和太平洋板块的交互处(图1),构造背景非常复杂,地质现象丰富,是研究和观测现代海底俯冲带过程的天然实验室[6, 11]。菲律宾海板块的东部和南部依次为伊豆-小笠原-马里亚纳海沟、雅浦海沟、帕劳海沟和阿玉海槽,菲律宾海板块的北部边界为东侧的南开(Nankai)海槽和西侧的琉球海沟,该板块西侧为菲律宾海沟[19]。基于构造重建,Hall[20]阐述了菲律宾海板块自50 Ma以来的构造演化。菲律宾海板块最初位于赤道附近,自新生代早期以来逐渐向北运动,在运动的过程中形成了西菲律宾海盆并伴随原(proto)伊豆-小笠原-马里亚纳岛弧的裂解作用。30~15 Ma,原伊豆-小笠原-马里亚纳岛弧发生裂解形成了帕里西维拉海盆和四国海盆。11 Ma,伊豆-小笠原-马里亚纳岛弧的岩浆活动再次活跃。5 Ma左右,随着伊豆-小笠原-马里亚纳海沟向太平洋板块方向的继续后撤,导致了马里亚纳海槽的打开,并活动至今[20-21]

    帕里西维拉海盆是菲律宾海板块的重要组成部分,位于九州-帕劳脊的东部,以索夫干断裂与北侧的四国海盆分开,南部边界为马里亚纳弧和雅浦岛弧,东界为西马里亚纳脊(图2)。帕里西维拉海盆呈狭长型,南北长约1 900 km,东西宽700 km,平均水深为4500~5 500 m,盆地中部为已经停止活动的帕里西维拉裂谷,水深最深处超过7 500 m。前人研究指出帕里西维拉海盆与四国海盆、马里亚纳海槽类似,是原伊豆-小笠原-马里亚纳俯冲带向海一侧后撤诱发的弧后扩张所形成的[11, 13, 25]。帕里西维拉海盆的扩张历史可以分为两个阶段,分别为第一阶段的东西向裂谷作用和海底扩张作用(开始于26 Ma左右),全扩张速率约为8.8 cm/a;第二阶段发生了逆时针的旋转,扩张轴的延伸方向由南北向变为北西-南东向,全扩张速率约为7.0 cm/a[26-29]。靠近帕里西维拉裂谷破碎带区域分布有一系列雁列式较短的一级构造片段,扩张停止的时间约为12 Ma[28]

    图  2  帕里西维拉海盆地质及建议钻探位置图
    前人研究的站位数据源自文献[6, 10, 22]。窗棂构造位置数据源自[23-24]。
    Figure  2.  Geology and proposed drilling positions (red and orange dots) in the Parece Vela Basin
    Data for previous drilling sites are from references [6,10, 22]. Data for mullion structures are from references [23-24].

    基于地质与地球物理学特征,本文将帕里西维拉海盆分为4个区域,分别为东区、西区、南区和裂谷区(图2)。其中,西区为帕里西维拉海盆中央裂谷以西至九州-帕劳脊的区域,东区为帕里西维拉海盆中央裂谷以东至西马里亚纳脊,裂谷区为帕里西维拉海盆的遗迹扩张中心区域,南区范围为北雅浦陡崖(North Yap Escarpment)以南至雅浦弧(图2)[30]。下面分别阐述这4个区域的地质与地球物理特征。

    帕里西维拉海盆西区的沉积物厚度较薄,大约为110 m,沉积物类型主要为远洋黏土、放射虫软泥和超微化石软泥。西区的地形比较复杂,有大量南北向排列的海山和深谷相间分布,在靠近九州-帕劳脊附近呈现凹陷的裂谷地形(图2)。帕里西维拉海盆的扩张速率约为7.7~8 cm/a[30]。西区中可以观测到振幅极小的磁异常,通常小于150γ,磁异常条带为5D-10(17~30 Ma),其中7-10号磁异常比较明显(7-10磁异常条带的波长较长不容易被后来的侵入体或者磁化的地形所掩盖),5D或5E的磁异常条带存在不确定性,这可能与扩张末期靠近扩张轴的洋脊跳跃有关[31-32]。DSDP449站位位于该区(图2),钻取了151.1 m,共获得岩心93.4 m,其中上部110 m为沉积层(远洋黏土、放射虫软泥和超微化石软泥),下部41.1m为枕状玄武岩和玄武岩熔岩流[17]。该区域的海底熔岩为玄武岩,具有类似于弧后盆地玄武岩(BABB)的微量元素特征和类似于印度洋型MORB的同位素特征[6, 33-34]

    帕里西维拉海盆东区的沉积物较厚,厚度从西马里亚纳脊附近的3 500 m向西递减到100 m左右,沉积物主要为远洋黏土和晚渐新世—晚中新世的火山碎屑,这些火山碎屑物质可能为西马里亚纳脊的火山活动的产物[32]。东区的地形比较平滑,未能识别出明显的磁异常,可能与沉积层较厚有关,水深约为4 500~5 500 m[11, 32]。东区现有3个钻孔站位(DSDP 53、54、450)和一个拖网站位(DM-1398)获取到了底质样品(图2)。DSDP 53站位的底部(约193 m)为侵入的火山岩体,上覆有远洋黏土、放射虫软泥和火山灰;DSDP 54站位在海底之下292 m处发现了玄武岩熔岩流,上覆有火山灰层。DSDP 450站位成功钻到了海水-沉积物界面之下340 m,上部33 m为沉积层,包括远洋黏土、玻屑凝灰岩以及细粒的玻屑凝灰岩,最下部7 m为枕状玄武岩,中部为火山玻璃凝灰岩[17]。基于底部玄武岩和上覆沉积物的接触关系的情况,说明仅有DSDP 54站位最下方的玄武岩可以代表基底。DM-1398站位获得了大量的海底熔岩样品,它们均为亚碱性玄武岩和辉长岩[22]。东区的海底熔岩具有类似于弧后盆地玄武岩(BABB)的微量元素特征和类似于印度洋型MORB的同位素特征[6, 33-34]

    帕里西维拉海盆南区的构造特征比较复杂(图2),海山、裂谷、丘陵等海底地貌单元相间分布,根据构造形态前人将其分为5个次级单元(A、B、C、D、E)[35]。A单元靠近雅浦岛弧,广泛分布有北西-南东向的丘陵,可能是帕里西维拉海盆第二阶段海底扩张的产物;B单元位于A单元西侧,与帕里西维拉海盆主体相连,该单元存在大量南北向展布的深海丘陵,可能是第一阶段海底扩张的产物;C单元位于B单元东南侧,广泛发育北东东-南西西向展布的深海丘陵,可能是海底扩张与裂谷体系相互作用的产物;D单元位于帕里西维拉海盆最南端,广泛分布有线性和圆锥形的海山;E单元位于B单元西南侧、靠近九州帕劳脊的位置,该单元分布有两个半月形深水裂谷,深度分别为6100和5 500 m[35]。南区未能识别出磁异常条带,水深范围为5200~500 m,水深从北向南逐渐变浅[35]。KH05-1-D1拖网站位取到了风化的枕状熔岩,可能为玻安岩或者岛弧拉斑玄武岩[35-36]。2019年自然资源部第一海洋研究所执行的CJ09航次对帕里西维拉海盆进行了电视抓斗取样,获得了多个站位的玄武岩样品。结果表明,帕里西维拉海盆南部玄武岩具有类似于N-MORB和IAB之间的微量元素特征和印度洋型MORB的同位素特征,其地幔源区中具有较高的含水量和氧逸度[18]。帕里西维拉海盆南部的东半部已缺失,其缺失的原因仍存在争议,目前有两种观点,一个是通过转换断层迁移到现今西马里亚纳弧西侧[31, 35],另一个观点认为是由于东侧卡罗琳板块的碰撞,导致了盆地东侧部分仰冲到雅浦弧地壳之上[30, 37]

    帕里西维拉海盆裂谷区是指已经停止活动的扩张中心区域(图2),其沉积物较薄,小于100 m。裂谷区的水深相对较深,最深处超过了7 500 m。裂谷区地形比较复杂,分布了大量的拆离断层、裂谷片段和核杂岩。每一个裂谷段都可以识别出窗棂构造,被解释为岩浆供给不足环境下大洋拆离断层的下盘[28]。在北纬16°附近发现了一个巨大的窗棂构造,被称为哥斯拉(Godzilla)窗棂构造(图2),它是世界上已知的最大的窗棂构造,比中大西洋中脊窗棂构造大了十多倍[28]。前人通过拖网和ROV(Remote Operated Vehicle,遥控无人潜水器)等取样技术在帕里西维拉裂谷获得了大量的蛇纹石化橄榄岩和辉长岩样品。这些橄榄岩分为3种类型,分别为F型(方辉橄榄岩)、P型(含斜长石的方辉橄榄岩和纯橄岩型的方辉橄榄岩)和D型(纯橄岩)[28, 38]。帕里西维拉裂谷橄榄岩最突出的特征是小尺度的肥沃型橄榄岩和难熔型橄榄岩的混合,其中肥沃型的橄榄岩是地幔橄榄岩经历低程度部分熔融(4%)的残余,纯橄岩和含斜长石的橄榄岩是不同比例熔体-地幔相互作用的产物[28, 38]

    尽管前人对帕里西维拉海盆进行了相应的研究,但是相较于菲律宾海板块中研究程度较高的西菲律宾海盆和马里亚纳海槽,帕里西维拉海盆的研究程度较浅,样品数量较少[39]。因此,帕里西维拉海盆仍存在如下几个亟待解决的关键科学问题:

    (1)帕里西维拉海盆扩张动力学过程。帕里西维拉海盆扩张停止的时间也存在争议,一部分学者基于磁异常条带认为帕里西维拉海盆海底扩张停止的时间为17 Ma[31],一部分学者基于磁异常条带和扩张速率认为海底扩张停止的时间为12 Ma[28],另一部分学者基于帕里西维拉裂谷的核杂岩数据推断扩张停止的时间为7.9 Ma[23]。上述观点都是基于地球物理资料得到的,缺少相应的基底玄武岩的K-Ar/Ar-Ar等高精度年龄数据。因此,建议在帕里西维拉海盆布置D-1、D-2、D-4站位来获取相应的基底岩石样品(图2)。这3个站位都是在帕里西维拉海盆西半部分靠近扩张轴的位置,这些位置的样品代表了帕里西维拉海盆弧后扩张活动晚期的产物,同时这些位置远离西马里亚纳脊,其沉积层较薄(明显低于东半部分的沉积物厚度),比较容易钻取到基底岩石样品。同时分别在靠近九州-帕劳脊和西马里亚纳脊处布置D-5和D-6站位,通过获取的基底岩石样品来限定帕里西维拉海盆开始扩张的时间。

    (2)海盆之下的地幔源区性质探讨。由于基底岩石样品缺乏,帕里西维拉海盆的地幔源区性质不清楚,帕里西维拉海盆的地幔是否存在不均一性仍不清楚。我们建议布置D-1、D-2、D-4站位来研究帕里西维拉海盆活动晚期的地幔性质及其地幔性质在纬度上是否存在不均一性(图2)。D-2、D-5、D-6站位的设置,主要是为了研究帕里西维拉海盆海底扩张从早期到晚期演化过程中地幔源区性质的变化,以及受俯冲组分影响程度是否与距离扩张中心距离有关。其中D-5和D-6的位置远离扩张轴,钻取的样品代表弧后扩张早期的产物;D-2靠近扩张轴,钻取的样品代表弧后扩张晚期的产物。

    (3)帕里西维拉海盆轴部少量海山的成因机制。帕里西维拉海盆属于西太平洋第二扩张幕的弧后盆地,其扩张时代与四国海盆、南海、苏禄海、日本海和鄂霍次克海相一致。在同时代的弧后盆地中南海和四国海盆的扩张中心处也分布有一系列的海山,但是它们的成因和形成年龄有较大的差别[29, 40-42]。南海扩张轴附近的海山是在南海停止扩张之后5 Ma出现的,其成因机制与海南地幔柱有关;四国海盆轴部的Kinan海山链是在海底扩张停止之后马上就形成的,可能是受到了EM1组分的影响[29, 40-42]。帕里西维拉海盆轴部海山的成因是类似于四国海盆的Kinan海山链还是南海扩张期后的海山还需要进一步研究。因此,D-3站位选定在帕里西维拉海盆轴部最大的一个海山上(图2),该海山顶部相对平坦,水深较浅(约为2 060 m),有利于获得更多的海山样品来研究其成因机制。

    (4)帕里西维拉海盆内核杂岩的成因机制。大洋核杂岩是指在构造拉张应力的作用下,地壳深部和上地幔物质发生去顶、抬升而形成的穹隆状构造岩石组合[43-44]。与拆离断层和大洋核杂岩有关的洋脊不对称扩张模式丰富和完善了海底扩张的新模式。大洋核杂岩和拆离断层主要分布于岩浆供给不充足的慢速和超慢速扩张脊,例如大西洋中脊、中印度洋中脊、东南印度洋脊和西南印度洋脊。Akizawa等[24]在四国海盆发现了玛多(Mado)窗棂构造和核杂岩,并指出在该窗棂构造处的大洋核杂岩在岩性和成分上类似于慢速-超慢速扩张洋中脊[24,45-48]。前人通过高精度的测深学研究,在帕里西维拉裂谷中部发现了巨大的哥斯拉(Godzilla)窗棂构造和核杂岩,出露的岩石类型主要为蛇纹石化橄榄岩和辉长岩[21]。帕里西维拉裂谷处的哥斯拉窗棂构造是全球已发现最大的窗棂构造,同时帕里西维拉扩张中心是少数中等扩张速率的洋中脊,对完善海底扩张理论具有重要的研究意义[21, 28]。但是目前仅有少量的拖网和ROV站位对该区域进行了调查取样,缺少相应的海底钻探站位来研究大洋岩石圈的组成和演化过程。同时,由于拆离断层的存在,帕里西维拉海盆的洋壳直接暴露在海底,有利于取样。因此,我们建议在哥斯拉窗棂构造处布置2个钻探站位(D-7和D-8站位),来获取帕里西维拉海盆洋壳的岩心样品(图2),通过研究获取的样品来探讨该核杂岩的成因机制。

    (5)沉积过程及古海洋古气候演化。帕里西维拉海盆是一典型边缘海盆,以IBM弧与开放大洋分割开来,其沉积物记录了丰富的地质作用信息,具有独特的地质意义。对上述建议钻探位置获取的沉积物样品开展研究,有助于理解该海盆的沉积过程、物源信息以及周围地质单元的岩浆活动规律,并可恢复古海洋、古环境及古气候演化历史。

  • 图  1   Caroline海盆在西太平洋中的区域位置、区域水深地形图

    不同颜色的点代表不同阶段的国际大洋钻探站位[1]

    Figure  1.   The bathymetry map of the western Pacific marginal seas and the location of the Caroline Sea

    Different colored dots represent drill sites from different stages of International Ocean Drilling Programs[1]

    图  2   Caroline海盆与邻域水深和构造单元图(a) 及Caroline海盆与邻域三维立体地形图(b)

    红色虚线A、B、C、D为建议的海底地震仪和海底大地电磁仪的剖面。测线A:过Ayu海盆;测线B:过Caroline海脊系统和Sorol海槽裂谷;测线C:过Eauripik海岭;测线D:过Mussau俯冲海沟和Lyra海槽,到达Ontong-Java大火成岩省

    Figure  2.   Bathymetric and tectonic map (a) and three-dimensional topographic map (b) of the Caroline Basin and its adjacent areas

    The red dashed lines A, B, C and D are designed profiles of ocean bottom seismic and submarine magnetotelluric surveys. Profile A: over the Ayu Basin; Profile B: over the Caroline Ridge system and Sorol Trough rifting system; Profile C: over the Eauripik Ridge; Line D: over the Mussau subduction trench and Lyra Trough, and reaching the Ontong-Java large igneous province

    图  3   研究技术路线图

    OBS:海底地震仪;OBEM:海底大地电磁仪

    Figure  3.   Technical flowchart

    OBS: Ocean Bottom Seismometer; OBEM: Ocean Bottom Electromagnetometer

    表  1   Caroline海盆研究现状

    Table  1   Current research status in the Caroline Basin

    研究者研究范围研究数据初步结论
    Weissel and Anderson, 1978[2]Caroline 海盆地震数据等存在独立 Caroline 海板块
    Gaina and Müller, 2007[3];Bracey, 1975[4];MacLeod et al., 2017[5]Caroline 海盆磁异常海盆扩张历史复杂,可能存在扩张中断、
    洋脊跃迁、重新活动
    Li and Wang, 2016[6]Caroline 海脊和
    Eauripik 海岭
    重磁、热流数据等两者地球物理场和深部结构差异大,不可能同源
    Erlandson et al., 1976[7];Weissel and
    Anderson, 1978[2];Hegarty et al., 1983[8]
    Mussau 俯冲海沟重力、水深数据等Mussau 海沟是初始俯冲的产物,
    俯冲程度由北向南加大
    Weissel and Anderson, 1978[2];Fujiwara et al., 1995[9];Fujiwara et al., 2000[10];Lee, 2004[11]Ayu 海盆水深数据等洋中脊年龄、海底扩张动力学机制未明
    Weissel and Anderson, 1978[2];Bracey, 1983[12]
    Li and Wang, 2016[8]
    Caroline 海脊及
    Sorol 海槽
    岩石地球化学、重磁、
    热流、水深数据等
    Sorol 海槽为斜向张裂转换系统;
    Caroline 海脊大陆边缘张裂演化模式
    Ryan, 1988[13];Tregoning and Gorbatov, 2004[14]新几内亚俯冲带地震层析成像活跃俯冲带,~9 Ma 以来 ~650 km 板片俯冲
    下载: 导出CSV
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  • 收稿日期:  2019-03-14
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