青藏高原东南缘陆地时变重力演化特征及等效源反演

doi:10.3969/j.issn.0253-4967.2025.01.015

摘要/Abstract

摘要：

文中利用青藏高原东南缘2014—2022年的陆地时变重力资料, 首先基于贝叶斯平差方法获取了研究区不同时间尺度的区域时变重力场演化特征, 继而采用球坐标系下的六面体单元构建等效源模型, 通过检测板模型测试对测网的场源分辨能力进行了评估, 并在场源分辨力较好的区域反演了与构造变化及地震孕育相关的等效场源体的视密度变化特征。利用该方法获取了地壳20km深度处等效源-1.2~1.2kg/m³的视密度变化, 约为正常地壳平均密度的0.4‰。受川滇块体主要活动断裂带控制, 视密度变化区域主要集中在川滇块体西边界的大理—乡城一带及川滇块体东边界的小江断裂带附近, 并揭示了漾濞 M_S6.4 地震及通海2次5级地震前的能量积累、震前地质运动活跃至震后能量释放视密度减弱物质调整的过程。长时间尺度的视密度增加是青藏高原东南缘物质持续S向或SE向挤出及壳内深部物质运移的共同结果, 其空间分布特征与前人获取的低速、高导区域一致。视密度的强、弱变化特征与同时期的地震时空强弱分布特征相对应, 且M≥5地震多发生在视密度增加区域边缘或正、负视密度过渡区域, 契合“震质源和震质中”原理。文中获得的多期场源视密度的变化, 可用于定量化地解释地质和地球物理结果, 提取与孕震相关的深部场源信号, 研究区域重力场变化与地壳深部的构造运动和变形活动的联系, 对于了解该地区的深部动力学过程具有深远意义。

关键词: 时变重力场, 位场反演, 视密度变化, M≥5.0地震, 贝叶斯平差

Abstract:

This study analyzes terrestrial time-varying gravity data from the southeastern margin of the Tibetan Plateau, covering the period from 2014 to 2022. Using the Bayesian adjustment method, we first captured temporal variations in the regional gravity field at different time scales. Then, the Tesseriod model was applied to simulate the field source medium and construct an equivalent source model. The gravity network's ability to resolve field sources was further evaluated using a checkerboard model. In regions with high source resolution, we inverted the apparent density variations of equivalent sources to examine tectonic changes and earthquake generation. The main findings are as follows:

1)The gravity network effectively reflects recent regional earthquakes(M≥5.0), with most events occurring in the centers of four quadrants of gravity variation or within high-gradient zones of positive and negative anomalies. 2)Analysis of the field source resolution capability, based on various checkerboard models, indicates that most areas of the gravity survey network have a resolution better than 1°×1°, except at the network edges. Notably, resolution improves to 0.5°×0.5° near the Dali, Anninghe-Zemuhe-Xiaojiang fault, and Xichang regions, along the boundary of the Grade I active block. 3)Long-term gravity field inversion results reveal apparent density changes ranging from -1.2kg/m³ to 1.2kg/m³ within 1km-thick equivalent layers at depths of up to 20km. This variation is approximately 0.4‰ of the average crustal density. Spatially, regions of increased apparent density correlate with active faults along the western boundary of the Sichuan-Yunnan block(near Dali-Xiangcheng)and the Xiaojiang fault zone on its eastern boundary. 4)Apparent density changes indicate energy accumulation preceding the Yangbi M_S6.4 earthquake and two M5.0 earthquakes in Tonghai. The data capture pre-earthquake tectonic activity and subsequent crustal adjustments that led to decreased apparent density post-earthquake. Energy accumulation for the Yangbi earthquake is inferred to have started in 2015, driven by southward extrusion of materials along the eastern edge of the Tibetan Plateau and deep crustal migration. The complex location of the epicenter—at the intersection of the Weixi-Qiaohou and Honghe fault zones—may explain the area's frequent seismicity. Moreover, this region is characterized by low velocity and high conductivity, suggesting that fluid-channel materials surged into the source area, reactivating previously unmapped faults and triggering the Yangbi earthquake. Apparent density changes along the southern Xiaojing fault zone similarly show stress accumulation before the Tonghai M5.0 earthquakes, followed by a notable post-earthquake decrease and a rising trend in density between 2021 and 2022. The southern Xiaojing fault zone thus warrants close monitoring as a significant earthquake-prone region. 5)The long-term increase in apparent density results from continued southward or southeastward material extrusion and deep crustal migration along the southeastern margin of the Tibetan plateau. The spatial distribution aligns with previously identified low-velocity and high-conductivity areas. 6)Apparent density fluctuations correspond to the spatiotemporal distribution of M≥5 earthquakes, with these events often occurring at the edges of regions with increased density or at transitions between positive and negative density zones, aligning with the “hypocentroid and epicentroid” principle.

In summary, this study documents gravity field and apparent density variations across the region, providing insights for quantitative interpretation in geological and geophysical research. These findings help identify deep field source signals associated with earthquake generation, reveal relationships between regional gravity field variation and tectonic movement, and offer a better understanding of dynamic process in deep crust in the Tibetan Plateau.

Key words: Time-varying gravity field, Potential field inversion, apparent density changes, M≥5.0, Bayesian adjustment

郑秋月, 陈政宇, 吴宇琴, 黄江培, 刘东, 王青华. 青藏高原东南缘陆地时变重力演化特征及等效源反演[J]. 地震地质, 2025, 47(1): 246-266.

ZHENG Qiu-yue, CHEN Zheng-yu, WU Yu-qin, HUANG Jiang-pei, LIU Dong, WANG Qing-hua. THE CHARACTERISTICS OF TERRESTRIAL TIME-VARYING GRAVITY CHANGES AND EQUIVALENT SOURCE INVERSION ON THE SOUTHEASTERN MARGIN OF THE TIBETAN PLATEAU[J]. SEISMOLOGY AND GEOLOGY, 2025, 47(1): 246-266.

图/表 10

图1 a 测区的地质构造; b 2014年以来M≥5.0地震活动分布

Fig. 1 Geological structure(a) and distribution of seismicity(b) of the survey area.

图2 云南及周边区域流动重力测网分布

Fig. 2 Mobile gravity network in Yunnan Province and its adjacent area.

图3 研究区检测板模型(a、c)及测点理论重力异常(b、d) 图a、b的分辨率为1°×1°, 图c、d的分辨率为0.5°×0.5°

Fig. 3 Theoretical gravity anomaly(b, d)of checkboard model(a, c).

图4 研究区含噪声的检测板模型测试 a 0.5°×0.5° 检测板; b 1°×1° 检测板

Fig. 4 Inversion results of checkboard model(0.5°×0.5° and 1°×1°)with noise.

表1 测网重力观测资料的平差结果

Table1 Bayesian adjustment results of gravity observation data from relative gravity network

测期	观测仪器	点值平均精度/μGal
2014-C1	CG-5(#1169, #1170, #217, #230); LCR-G(#132, #843)	7.2
2014-C2	CG-5(#1169, #1170, #217, #230); LCR-G(#132, #843)	6.3
2015-C1	CG-5(#1169, #1170, #1229, #1235); LCR-G(#132, #843)	6.9
2015-C2	CG-5(#1169, #1170, #1229, #1235); LCR-G(#132, #843)	5.7
2016-C1	CG-5(#1169, #1170, #1229, #1235); LCR-G(#132, #843)	7.0
2016-C2	CG-5(#1169, #1170, #1229, #1235); LCR-G(#132, #843)	6.3
2017-C1	CG-5(#1169, #1170, #1427, #1235); LCR-G(#132, #843, #854, #003, #829)	8.2
2017-C2	CG-5(#1169, #1170, #1427, #1235); LCR-G(#053, #057)	7.7
2018-C1	CG-5(#1169, #1170); LCR-G(#149, #150, #132, #843)	6.0
2018-C2	CG-5(#1169, #1170, #834, #845); LCR-G(#149, #150)	7.8
2019-C1	CG-5(#1169, #1170, #834, #845); LCR-G(#149, #150)	7.0
2019-C2	CG-5(#1169, #1170, #834, #845); LCR-G(#149, #150)	8.0
2020-C1	CG-5(#1169, #1170); LCR-G(#149, #150)	6.9
2020-C2	CG-5(#1169, #1170); LCR-G(#149, #150)	5.7
2021-C1	CG-5(#1169, #1170, #097, #098); LCR-G(#149, #150)	9.5
2021-C2	CG-5(#1169, #1170, #097, #098); LCR-G(#149, #150)	10.2
2022-C1	CG-5(#1169, #1170, #097, #098); LCR-G(#149, #150)	9.7
2022-C2	CG-5(#1169,#1170);LCR-G(#149,#150)	8.2

图5 贝叶斯平差获取的2014—2022年区域重力场2年期差分动态变化特征

Fig. 5 Variation characteristics of regional gravity field with two-year differences after Bayesian adjustment from 2014 to 2022.

图6 2014—2016年区域重力场累积变化特征

Fig. 6 The regional cumulative gravity field changes from 2014 to 2016.

图7 2016—2022年区域重力场累积变化特征

Fig. 7 The regional cumulative gravity field changes from 2016 to 2022.

图8 青藏高原东南缘2015—2022年的累积视密度变化特征

Fig. 8 Cumulative apparent density variations in the southeastern margin of the Tibetan Plateau from 2015 to 2022.

图9 青藏高原东南缘下地壳速度 a 接收函数与面波联合反演得到的21km深度处的S波速度(修改自Bao et al., 2015); b 体波与面波联合反演得到的20km深度处的S波速度(修改自刘影等, 2023)

Fig. 9 Lower crustal velocities beneath the southeastern margin of the Tibetan Plateau.

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