Deep Seismic Evidence of Cenozoic Tectonic Migration in the Western Pacific Back-Arc Area
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摘要: 为了研究西太平洋弧后边缘海盆地的深部构造特征，于2015年在东海琉球岛弧弧后地区布设了一条穿过东海陆架盆地、钓鱼岛隆褶带、南冲绳海槽地区和琉球岛弧的主动源广角反射/折射深部地震剖面.利用走时正演和反演的方法得到的二维速度结构模型展现了西太平洋边缘弧后地区莫霍面的深度由东海陆架地区的大于30 km显著抬升至南冲绳海槽轴部的约16 km，地壳高度拉张减薄，并存在一系列显著的不连续下地壳高速体，速度达6.8~7.3 km/s，这是地幔上涌的显著表现.模型从深部结构角度展现了新生代以来西太平洋弧后盆地扩张中心的变迁，证实了西太平洋洋陆过渡带内深部上涌的软流圈在弧后拉张过程中不断地向洋跃迁，形成自西向东的构造迁移，并带动岩石圈进行幕式伸展，认为新生代向洋变新的构造迁移是太平洋俯冲带后撤引起的一系列弧后深-浅部地球动力效应.Abstract: To study the deep crust structure in the back-arc area, we present an active source wide-angle reflection/refraction profile in the back-arc area of Ryukyu Island in the East China Sea in 2015, which passed through the East China Sea shelf basin, the Diaoyu island uplift belt, the southern Okinawa Trough and the Ryukyu Island arc. The 2D velocity structure model obtained by forward modeling and travel tomographic shows that the depth of Moho rises significantly from more than 30 km in the East China Sea shelf to about 16 km in the axis of the Okinawa Trough, and the crustal thickness decreases significantly. A series of discontinuous high-velocity zones with velocity 6.8-7.3 km/s were identified in the lower crust of the back-arc region, which is a remarkable manifestation of mantle upwelling. From the perspective of deep crustal structure, the model clearly shows the tectonic migration from west to east in the back-arc area of the Western Pacific since Cenozoic and confirms that the as thenosphere upwelling in the deep part of the Western Pacific oceanic-continental transition zone transits continuously to the ocean during the back-arc spreading process, forming the tectonic migration from west to east, and driving the episodic extension of the lithosphere. We believe that the Cenozoic tectonic migration to the ocean is a series of back-arc deep-shallow geodynamic effects caused by the retreat of the Pacific subduction zone.
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图 1 （a）西太平洋构造简图; （b）东海及邻区构造区划图
a.红框内显示为b的位置; b.黑色实线代表放炮测线，黄色圆圈代表OBS，红色圆圈代表丢失OBS
Fig. 1. a) Plate tectonic context of the Western Pacific Ocean; (b) Overview map of the East China Sea and adjacent area (study area)
图 2 （a）OBS10站位垂直分量地震记录剖面；（b）射线追踪情况；（c）走时拟合情况
a.位置见图 1，折合速度6 km/s，台站位置见图 1；c.展示了观测走时(彩色)和最终速度模型的计算走时（黑线）, 下地壳折射波震相Pg2视速度范围为6.8~8.0 km/s，是高速地幔物质侵入地壳的反映，折合走时表示为原始走时T-offset/折合速度
Fig. 2. (a)Seismic profile of the vertical component of OBS10; (b)The ray paths in the forward model; (c) The travel time fits between calculated (solid black lines) and observed(colored lines)
图 4 (a) OBS2015正演P波速度模型；(b)射线密度模型；(c)走时拟合结果
a.模型自西向东依次为浙闽隆起、东海陆架盆地、钓鱼岛隆褶带和琉球隆起, 红色点代表反射震相(PcP, PmP)控制的反射界面; b.空白处为无约束区域，射线覆盖次数由绿向红逐渐增加; c.展示了模型中识别出的所有震相的实测走时（彩色）与理论计算走时（黑色），蓝色圆圈为OBS
Fig. 4. (a)Results of the OBS2015 profile forward-velocity Ray Invr model; (b) Ray coverage density throughout the model; (c) All picked(colors) and calculated (black dots) travel times of the same phases for all of the receivers in the model
图 5 OBS2015测线反演最终模型（a）和射线密度图（b）
蓝色圆圈为OBS
Fig. 5. (a)Result of the OBS2015 profile travel time inversion using the code Tomo2D; (b) The derivative weight sum (DWS)
图 6 东海弧后盆地扩张动力学机制模型
灰色箭头代表新生代早期扩张中心；黑色箭头代表现今弧后扩张中心；紫色区域代表下地壳高速体
Fig. 6. Dynamic mechanism model of east China sea back-arc basin expansion
图 7 东海弧后扩张演化与构造迁移示意图
a.东海地区新生代以来构造演化剖面图; b.东海地区弧后盆地扩张中心迁移图
Fig. 7. Sketch map of back-arc spreading evolution and tectonic migration model of the East China Sea
表 1 东海陆架盆地与冲绳海槽盆地构造演化阶段对比
Table 1. Comparison of tectonic evolution stages between East China Sea shelf basin and Okinawa Trough basin
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