3D P-wave velocity structure beneath Ordos block and its surrounding regions and its tectonic implications
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摘要: 利用中国地震科学台阵密集流动地震台站和固定地震台站记录的远震P波资料，采用走时层析成像方法反演获得了鄂尔多斯及周边地区上地幔的精细速度结构。结果显示，鄂尔多斯地块下方存在较厚的高速异常，其中西部深度约为180 km，北部约为150 km，中部的局部地区可达300 km，表明鄂尔多斯地块总体上仍保持克拉通特性。鄂尔多斯地块北部相对较薄的岩石圈可能与地幔物质上涌对岩石圈进行了加热和改造有关，其西部岩石圈的减薄可能与青藏高原东北缘上地幔热物质的横向扩展有关。华北克拉通东部地块、中部地块及鄂尔多斯地块东北部的上地幔表现出大范围的低速异常，推测可能与太平洋板块后撤导致的伸展构造背景、滞留板片脱水以及板片前缘局部对流有关。在该地区的伸展背景下，岩石圈或软流圈的熔融物沿着软弱带上涌并形成了包括大同火山在内的火山群。Abstract: We obtain a high-resolution velocity structure of the upper mantle in the Ordos block and its surrounding regions by travel-time tomography, using the teleseismic P-wave data recorded by dense temporary stations of China Seismic Array and permanent stations. The results show a thick high-velocity anomaly beneath the Ordos block, which extends to a depth of about 180 km in the west, 150 km in the north, and up to 300 km in part of the central area, indicating that the Ordos block still maintains craton stability as a whole. The relatively thin lithosphere in the northern Ordos may be related to the heating and modification of the lithosphere by the mantle upwelling, whereas the lithosphere thinning in the western Ordos may be associated with the lateral expansion of the warm upper mantle of northeastern Tibet. The upper mantle of the eastern North China Craton, the central North China Craton and the northeastern Ordos block exhibit broad low-velocity anomalies, which may be related to an extensional tectonic setting caused by the rollback of Pacific Plate, the dehydration of the stagnant slab and the local convection at the front edge of the slab. In extensional environments, melts from the lithosphere or asthenosphere upwelled along the weak zone and formed volcanoes including Datong volcano.
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Keywords:
- Ordos block /
- upper mantle structure /
- seismic tomography /
- North China Craton /
- mantle upwelling
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图 5 研究区不同深度h处的横切片P波速度结果
Figure 5. P-wave velocity images in map view at the different depths h in the studied area
（a） h＝50 km；（b） h＝120 km；（c） h＝190 km；（d） h＝270 km；（e） h＝350 km； （f） h＝440 km；（g） h＝530 km；（h） h＝620 km；（i） h＝710 km
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图 1 研究区构造背景及地震活动性
圆点表示1970年1月至2020年12月的M≥3.0地震。新生代玄武岩位置修改自Liu和Ying （2020）及邹和平等（2010）
Figure 1. Tectonic background and seismicity in the study area
The dots indicate earthquakes with magnitude M3.0 or higher from January of 1970 to December of 2020 in the studied area. The locations of the Cenozoic basalts are modified from Liu and Ying （2020），Zou et al （2010）
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图 2 台站（a）及地震震中（b）分布图
图（a）中实线为构造边界，虚线为南北重力梯度带，倒三角形表示固定台站，三角形表示中国地震科学台阵三期流动台阵；图（b）中圆点为地震，星形为研究中心
Figure 2. Distribution of stations （a） and epicenters （b）
In Fig. （a），solid lines delineate the tectonic units，the dashed line is the north-south gravity gradient zone，the inverted triangles indicate permanent stations，and the triangles indicate the temporary stations of phase III of the ChinArray Project；In Fig. （b），the dots denote the earthquakes，and the star denotes the center of studied region
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图 3 原始走时残差与相对走时残差的对比（a）及光滑和阻尼因子测试（b）
Figure 3. Comparison of the raw travel time residuals with relative ones （a） and trade-off curves for the norm of solution and RMS （root-mean-square） travel time residual （b）
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图 4 不同深度h下0.5°×0.5°网格检测板结果
Figure 4. Results of checkerboard test for 0.5°×0.5° grid spacing with different depths h
（a） h＝50 km；（b） h＝120 km；（c） h＝190 km；（d） h＝270 km；（e） h＝350 km；（f） h＝440 km；（g） h＝530 km；（h） h＝620 km；（i） h＝710 km
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图 6 纵剖面位置（a）及其P波速度结果（b−e）
图（b）−（e）中，虚线代表410 km及660 km间断面
Figure 6. Location of the four vertical cross sections （a） and P-wave velocity results along the sections （b−e）
The dashed lines represent the 410 km and 660 km discontinuities in Figs. （b）−（e）
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图 7 恢复性分辨率试验结果
（a） 异常输入分布，图中HV1和HV2代表3%高速异常，LV1和LV2代表−3%低速异常，分别用蓝色和橘色方框表示，且LV2和HV2在116°E以东重合；（b，d） 输入模型；（c，e） 输出模型
Figure 7. Restoring resolution test results
（a） The distribution of input anomalies，where HV1 and HV2 denote 3% high anomalies，and LV1 and LV2 denote −3% low anomalies，noting that LV1 and LV2 overlap to the east of 116°E；（b，d） The input models；（c，e） The output models
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