Morphological structure of stagnant slab under southern Japan and Ryukyu Island Arc based on seismic waveform fitting
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摘要:
在日本南部及琉球岛弧地区，太平洋板块和菲律宾海板块共同向欧亚板块下方俯冲，形成复杂的双板块俯冲系统。滞留板片在地幔过渡带内的形态特征及其与地幔物质的相互作用影响着东海陆架盆地及中国大陆边缘的构造演化过程。本研究基于中国国家数字台网记录的发生于伊豆—小笠原地区的一次深源地震的宽频带波形资料，通过P波三重震相拟合，获得了日本南部及琉球岛弧下方660 km间断面附近的速度结构特征。结果显示，研究区域660 km间断面上方普遍存在高速异常体，其深度范围约为490—720 km，P波速度异常1.0%—3.0%；660 km间断面下沉深度为20—60 km，呈现出由南向北逐渐减小的趋势，速度跃变1.5%—3.0%。相较于前人基于地震活动性和层析成像的结果，本文高速异常体的存在位置要深于菲律宾海板块俯冲所能到达的地幔转换区上边界附近，因而其应为俯冲滞留的西太平洋俯冲板片物质，与菲律宾海板块俯冲物质无关；此外，660 km间断面较大的南北下沉深度变化应由俯冲板块带来的滞留物质及其引起的温度异常和相关的相变所导致。
Abstract:Under southern Japan and Ryukyu Island Arc, the Pacific plate and the Philippine Sea plate both subducted under the Eurasian plate, forming a complex double-plate subduction system. Statistical results of seismic activity reflect that there are significant differences in the influence of the two subducted plates on the mantle transition zone. It is currently unclear whether the stagnant slab beneath this region is a single Pacific plate or a mixed stagnant body consisting of the Pacific plate and the Philippine Sea plate. The properties, geometric characteristics, and morphological changes, as well as its interaction with the mantle material, collectively affect the tectonic evolution of the East China Sea Shelf Basin and the Chinese continental margin. The accumulation of the stagnant slab within the mantle transition zone and its interaction with the mantle material can cause variations in the depth of the 660 km discontinuity at the bottom of the mantle transition zone. Cold stagnant slab material induces depression of the 660 km discontinuity. By studying the depth of the 660 km discontinuity and its nearby velocity structure, we can explore the depth variation characteristics of the stagnant slab in the mantle transition zone beneath the southern Japan and Ryukyu Island Arc, obtain the lateral differences of the plate subduction process. This will deepen our understanding of the integrity of plate subduction in the Northwest Pacific Ocean and contribute to the study of the geodynamic processes of plate subduction. When the seismic wave passes through the 660 km discontinuity, the triplicated seismic phases will be generated. Utilizing the arrival times and amplitude characteristics of the triplicated waveforms recorded by a dense seismic network, we can effectively constrain the morphology of the discontinuity and the velocity structure near it.
In this study, we selected a deep earthquake that occurred in the Izu-Bonin recorded by the China National Seismic Network （CNSN）. The earthquake had a focal depth of 472 km, which avoided the influence of the triplicated waveforms associated with the 410 km discontinuity. The surface projections of the P-wave turning points are located in the southern Japan and Ryukyu Island Arc, and the characteristics of the triplicated waveforms can be used to constrain the depth of the 660 km discontinuity and its nearby velocity structure. Through identification and analysis of the morphological characteristics in P-wave triplicated waveforms, we divided the study area into 13 profiles, delineating horizontal differences in velocity structures based on distinct features of triplicated waveforms features. Building upon previous research findings and the characteristics of observed waveforms, we constructed a foundational velocity structure model. Employing a grid search methodology, we generated various parameter models. Theoretical seismic waveforms were subsequently computed using reflectivity method and compared against observed waveforms. The optimal velocity structure was determined via maximization of cross-correlation coefficients. Specifically, during the fitting process of P-wave triplicated waveforms, we refined waveform selection to minimize interference from non-triplicated waveforms, thereby augmenting fitting precision.
Our results reveal that: ① There is a high-velocity layer above the 660 km discontinuity with depth of 490−720 km and P-wave velocity anomaly of 1.0%−3.0%; ② The 660 km discontinuity depressed 20−60 km with velocity increment of 1.5%−3.0%, and the depression depth gradually decreases from south to north.
Drawing on insights gleaned from seismic tomography and tele-seismic data, we propose that the thickness of the high-velocity anomaly layer above the 660 km discontinuity significantly surpasses that of the subducting Pacific slab. This discrepancy likely arises from the halting of the downward motion of the subducted oceanic slab within the mantle transition zone by the 660 km discontinuity. This interruption triggers a lateral shift in motion, leading to the entrapment and subsequent buildup of the slab material within the mantle transition zone. Moreover, compared to previous studies based on seismic activity and tomography, our findings position the high-velocity anomaly layer at a depth deeper than typically reachable by the subduction of the Philippine Sea Plate, suggesting its composition primarily comprises material from the stagnant western Pacific slab rather than from the Philippine Sea Plate. Additionally, the depression of the 660 km discontinuity ranges from 20 to 80 km, exceeding depths attributed solely to thermal anomalies. We suggest that this depression may also involve phase transformations within the stagnant material brought by the subducted slab. The gradual reduction in depression depth from south to north likely reflects variations in subduction dynamics along the north-south direction.
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图 1 本文所用地震事件位置和台站分布图
黑色三角形为台站位置，按方位分布划分为13个剖面（A，B，···，M），红色三角形为剖面H上观测到到时延迟的台站；红色圆点为P波射线拐点的地表投影，黑色虚线为俯冲太平洋板片与菲律宾海板片等深线（Gudmundsson，Sambridge，1998）。右下角插图为660 km间断面附近三重震相射线路径图，包括地震射线AB，BC和CD
Figure 1. Location of the earthquake event and stations used in this study
Black triangles denote the used stations，and the studied region is divided into 13 profiles （A，B，···，M）. Red triangles in the profile H are the stations with obvious observed time delay. Red dots are the surface projections of P-wave turning points. Contours shown in black dashed lines represent the Pacific and Philippine Sea slabs （Gudmundsson，Sambridge，1998）. The bottom right inset shows ray paths of the triplication near the 660 km discontinuity，including the seismic rays AB，BC and CD
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图 2 剖面A观测波形与模型参数定义图
（a） 剖面A上的观测波形及与IASP91模型对应的走时曲线；（b） 前人参考模型M3.11 （Tajima，Grand，1995）及本文构建模型参数定义图。d1 （480—600 km）表示660上方高速异常体起始深度，d2 （490—720 km）表示最大速度异常所处深度，d3 （660—760 km）表示660深度，s2 （0—4%）表示高速异常最大速度异常扰动量，s3 （0—5%）表示660的速度异常跃变值
Figure 2. The observed waveforms of the profile A and the parameter definition diagrams of the model
（a） The observed waveforms of the profile A and the travel time curves calculated with the IASP91；（b） Predecessor reference model M3.11 （Tajima，Grand，1995） and the parameter definition diagrams of the model used in the grid search procedure. d1 （480—600 km） is the starting depth of the high-velocity layer above the 660，d2 （490—720 km） is the depth at which the maximum velocity anomaly occurs，d3 （660—760 km） is the depth of the 660，s2 （0—4%） is the maximum velocity anomaly of the high-velocity layer，s3 （0—5%） is the velocity anomaly of the 660
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图 3 剖面A波形拟合结果及互相关系数等值线图
（a） P波速度结构；（b） 波形拟合结果。绿线表示由最佳模型计算得到的走时曲线，紫虚线框标记用于计算互相关系数的波形；（c） 660 km间断面深度与速度异常的互相关系数等值线图。下同
Figure 3. Waveform fitting results and cross-correlation coefficients contour map of profile A
（a） P-wave velocity structure；（b） Waveform fitting results. The green line represents travel time curve calculated with the best model. The purple dotted frame marks the waveforms used for calculating the cross-correlation coefficients；（c） Contour map of cross-correlation coefficients of the 660 km depth and velocity anomaly. The same below
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图 15 剖面M波形拟合结果及互相关系数等值线图
Figure 15. Waveform fitting results and cross-correlation coefficients contour map of profile M
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图 4 剖面B波形拟合结果及互相关系数等值线图
Figure 4. Waveform fitting results and cross-correlation coefficients contour map of profile B
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图 5 剖面C波形拟合结果及互相关系数等值线图
Figure 5. Waveform fitting results and cross-correlation coefficients contour map of profile C
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图 6 剖面D波形拟合结果及互相关系数等值线图
Figure 6. Waveform fitting results and cross-correlation coefficients contour map of profile D
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图 7 剖面E波形拟合结果及互相关系数等值线图
Figure 7. Waveform fitting results and cross-correlation coefficients contour map of profile E
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图 8 剖面F波形拟合结果及互相关系数等值线图
Figure 8. Waveform fitting results and cross-correlation coefficients contour map of profile F
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图 9 剖面G波形拟合结果及互相关系数等值线图
Figure 9. Waveform fitting results and cross-correlation coefficients contour map of profile G
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图 11 剖面I波形拟合结果及互相关系数等值线图
Figure 11. Waveform fitting results and cross-correlation coefficients contour map of profile I
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图 12 剖面J波形拟合结果及互相关系数等值线图
Figure 12. Waveform fitting results and cross-correlation coefficients contour map of profile J
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图 13 剖面K波形拟合结果及互相关系数等值线图
Figure 13. Waveform fitting results and cross-correlation coefficients contour map of profile K
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图 14 剖面L波形拟合结果及互相关系数等值线图
Figure 14. Waveform fitting results and cross-correlation coefficients contour map of profile L
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图 10 剖面H波形拟合结果及互相关系数等值线图
Figure 10. Waveform fitting results and cross-correlation coefficients contour map of profile H
表 1 各剖面速度模型
Table 1 The velocity models of each profile
剖面 高速异常体
起始深度/km高速异常体最大
速度异常深度/km高速异常体最大
速度异常660 km间断面
深度/km660 km间断面
速度跃变A 600 650 1.0% 710 2.0% B 540 640 1.0% 720 3.0% C 600 680 2.0% 720 3.0% D 580 670 2.0% 710 3.0% E 580 680 2.0% 710 3.0% F 560 560 1.0% 700 2.0% G 490 640 1.0% 710 2.0% H 600 610 2.0% 705 1.5% I 550 550 2.0% 705 1.5% J 560 600 3.0% 690 1.0% K 490 630 1.0% 685 2.5% L 530 650 1.0% 680 3.0% M 530 660 1.0% 680 3.0% 
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