Constrained Inversion of Audio Magnetotelluric for Identifying Strata: A Case Study in Hami Basin
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摘要: 覆盖区地质填图是新时期地质填图的重要方向.音频大地电磁法（AMT）是覆盖区地质填图的重要地球物理方法之一，可以为地层和基岩面的刻画提供电性参数的约束.然而，常规的AMT反演无法精确刻画电性异常体的边界，且当缺乏其他地质与地球物理资料约束时，难以进行地质解译.针对此问题，基于数值模拟结果的可行性，利用哈密烟墩戈壁覆盖区的4条实测AMT剖面探讨了AMT约束反演在地层识别中的应用效果.相位张量分析指示研究区浅部（> 1 Hz）电性结构表现为二维特征，深部受三维结构影响；浅部为低阻，深部电阻率逐渐升高.采用不加约束二维反演获得了4条剖面的地下（< 3 km）电性结构.基于研究区的重力异常、地震解译结果、物性和钻孔资料，在二维反演结果上初步划分了渐新统-中新统和侏罗系地层的底界面；进而以这两个界面建立先验模型，并根据物性资料设置电阻率变化范围，进行AMT约束反演，获得了更优化的反演结果以及清晰可靠的渐新统-中新统和侏罗系的底界面.结果显示，研究区渐新统-中新统地层电阻率值略小于10 Ω•m，其底界面平均埋深为120 m；侏罗系电阻率值为10~100Ω•m，其底界面最深可达2 km.基岩面（侏罗系底界面）埋深整体上呈现为东南深、西北浅，这指示哈密烟墩地区中生代以来的沉积中心在东南部；此外，侏罗系地层与下伏的古生界地层存在角度不整合.研究表明，哈密烟墩地区新生代以来可能受到了近南北向应力挤压，在研究区中部形成近东西或北东东向的侏罗系隆凹相间的构造地貌格局.而渐新统-中新统地层底部的不整合面可能反映了后期褶皱构造的影响，这种隆凹作用相伴的褶皱构造可能具有同沉积性质.Abstract: Geological mapping on covered area is a crucial research of new geological mapping. Audio magnetotelluric (AMT) is one of effective geophysical methods for geological mapping on covered area, which can provide the constraint of electrical parameters for depicting strata and bedrocks. However, conventional AMT inversion cannot accurately describe the boundaries of electrical anomalies, and it is difficult to perform geological interpretation when there is no other geological and geophysical data constraints. Based on the feasibility of numerical simulation results and four AMT profiles in the Gobi desert area of Hami Yandun, it tries to investigate the availability of constrained AMT inversion in strata identification. Phase tensor analyses indicate that the shallow (< 1 Hz) electrical structure is mainly two-dimensional (2D), while the deep is affected by 3D structure. The resistivity is low in the shallow and gradually increases in the deep. The underground electrical structures of four profiles were obtained by 2D unconstrained inversion. Based on gravity anomalies, seismic interpretation results, physical properties of rocks and borehole data in the research area, the bottom interfaces of Oligocene-Miocene and Jurassic strata were preliminarily divided from the 2D inversion results. Furthermore, a prior model was established using the two interfaces, where the resistivity change ranges were set according to physical property data. Then, constrained AMT inversion was carried out. The better inversion results and the clear and reliable bottom interfaces of Oligocene-Miocene and Jurassic were obtained. Research results show that the resistivity of Oligocene-Miocene stratum is slightly smaller than 10 Ω•m and the bottom interface is shallow with an average depth of 120 m. The resistivity of Jurassic stratum is about 10-100 Ω•m and the bottom interface is deep up to 2 km. The buried depth of bedrock surface (Jurassic bottom interface) is deep in the southeast but shallow in the northwest, which indicates that the sedimentary center since Mesozoic is in the southeast of Hami Yandun area. Moreover, an angular unconformity exists between Jurassic and underlying Paleozoic strata. The study supports that Hami Yandun area may go through the extrusion from nearly NS compression stress since Cenozoic, resulting in the morphotectonic pattern of Jurassic uplift and depression with nearly EW or NEE direction in the central part. Besides, the angular unconformity beneath the Oligocene-Miocene strata may reflect the influence of later fold structure. This kind of fold structure along with uplift and depression might have the synsedimentary property.
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图 1 起伏界面数值模型反演结果
a. 正演理论模型；b. 不加约束反演，拟合差为2.58；c. 约束反演，拟合差为1.00；图中黑色三角为大地电磁测点，黑色线条为电性起伏界面
Fig. 1. Inversion results of numerical model on undulating interface
图 2 东天山区域（a）及哈密盆地研究区（b）
Fig. 2. Overview of the East Tianshan (a) and research region of Hami basin (b)
图 3 烟墩研究区测线、测点分布
底图为该区域布格重力异常图；黑色实心点为AMT测点；黄色实心点为典型测点；蓝线为地震测线；ZKY11和ZKY12为地震测线上的两个钻孔
Fig. 3. Survey lines and sites distribution in the research region
图 6 213.64 Hz (a)、62.15 Hz (b)、2.84 Hz (c)和0.61 Hz (d)四个频率的相位张量椭圆平面图
Fig. 6. Phase tensor ellipses for 213.64 Hz (a), 62.15 Hz (b), 2.84 Hz (c) and 0.61 Hz (d)
图 7 地层识别和提取分布流程
Fig. 7. Flowchart of formation identification and extraction distribution
图 8 AMT剖面的二维反演结果
蓝线和黑线分别表示初步解译的渐新统‒中新统底界面和侏罗系底界面
Fig. 8. Two-dimensional inversion results of AMT profiles
图 9 剖面1实测（上）与反演预测（下）的TE、TM模式视电阻率相位拟断面图
Fig. 9. Pseudo section diagrams of the apparent resistivity phase in TE and TM modes of profile 3 observed (top) and inversion prediction values (bottom)
图 10 研究区钻孔揭示的渐新统‒中新统底界面埋深
黑点为AMT测点，蓝线为地震测点，红十字代表研究区内的钻孔点位
Fig. 10. Buried depth of the bottom interface of Oligocene-Miocene stratum from boreholes in the research area
图 11 研究区地震剖面解译图
ZKY211和ZKY212为地震剖面上的两个钻孔；淡蓝色线代表第四系和渐新统‒中新统地层；绿线和深蓝色线代表侏罗系地层内部分界面；紫线代表侏罗系地层的底界面；黄三角和红三角分别代表两个钻孔下方渐新统‒中新统和侏罗系地层的底界面；Q.第四系；E3N1.渐新统‒中新统；J2t.中侏罗统头屯河组；J2x.中侏罗统西山窑组；D.泥盆系
Fig. 11. Seismic imaging results in the research area
图 14 渐新统‒中新统（a）和侏罗系（b）底界面埋深的平面分布图及凹陷的平面分布
图中圆圈填充颜色指示约束反演得到的渐新统‒中新统地层底界面埋深，红十字代表钻孔点位及下方的渐新统‒中新统地层底界面埋深，蓝色椭圆区域是划分的凹陷区域
Fig. 14. Depth distributions of the bottom interfaces of Oligocene-Miocene (a) and Jurassic (b), the distribution of depressions in the research area
图 15 研究区大地电磁剖面揭示的侏罗系厚度分布趋势与褶皱构造
Fig. 15. Thickness distribution and fold structure of the Jurassic strata revealed by magnetotelluric in the research area
表 1 烟墩地区岩石电阻率按地层划分的统计结果
Table 1. Statistic results of rock resistivity by stratification in Yandun area
系/统 地层代号 岩性 电阻率统计级别 渐新统‒中新统 E3N1 泥质砂岩 低阻（< 20 Ω•m） 侏罗系 J 砂岩 中阻（> 100 Ω•m） 泥盆系 D 闪长玢岩/花岗岩 高阻（> 1 000 Ω•m） 
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