大地电磁测深拟地震时间剖面解释法研究
|
摘要
大地电磁测深拟地震解释法是依据电磁波和弹性波在数学表达形式上和物理意义上都有一定的相似性原则,把地震法中行之有效的方法来用运到电磁法中的一种电磁解释方法。大地电磁测深拟地震时间剖面解释方法,在一维水平均匀层状介质条件下能有效地划分反射界面和电性层位,较之常规解释方法具有自己的特点,但是拟地震解释法和其它地球物理勘探方法的反演方法一样,都存在解的非唯一性。因此,如何缩小和判断解的非唯一性、提高解的精度和可靠性,取得更接近真实的地球物理模型,就成了拟地震解释法一项亟待研究的课题。
本文首先概述了大地电磁测深的发展概况及其数据处理的方法技术,重点阐述了大地电磁测深和地震勘探法的相关技术,论述了拟地震解释法的基本原理;推导了一维断面模型下拟地震法的反演计算公式,编写出了计算拟地震反射系数的程序;论文计算了一维两层、三层和四层不同模型参数的反射系数,说明在一维水平均匀层状介质条件下,大地电磁测深拟地震时间剖面解释方法能有效地划分反射界面和电性层位。
论文又从拟地震法中“微层”入手,探讨“微层”对反演结果的影响规律,以一维两层、三层和四层为模型,通过取不同厚度“微层”,反演计算反射系数,总结了不同厚度“微层”,对反演结果影响的基本规律是:1、相同模型不同厚度“微层”参数,其反演结果不尽相同;2、“微层”厚度划分越细,反演的结果与实际越接近;3、“微层”厚度越细,反演计算时间越长,成本增高;4、第一层电性层至少划分为两个“微层”,这样才能保证反演结果的正确性。
论文通过计算不同模型参数的反射系数的变化规律,论证在一维水平均匀层状介质条件下,大地电磁测深拟地震时间剖面解释方法能有效地划分反射界面和电性层位。同时,论文又通过“微层”厚度对反演计算结果的影响规律探讨,论证了“微层”厚度是影响拟地震解释法解的非唯一性的关键技术之一,科学合理选择“微层”厚度参数是提高解的精度和可靠性,实现反演更接近真实的地球物理模型的基础。
The pseudo - seismic interpretation is the method of to draw up the earthquake to explain the method deeply according to the similar to flexible wave express the formality and the physics meanings in mathematics top certainly all have principle of electromagnetic wave, valid method go in the earthquake method to use to carry the electromagnetism method of a kind of electromagnetism explain the method. The pseudo - seismic interpretation , can divide the line to reflect the interface availably under the condition of 1D , compared with the normal regulations that it have its own characteristics , but the pseudo - seismic interpretation like other Earths physics methods all exist fault. Therefore, how contract and judge the fault and raise the accuracy and credibility of the solution, becoming a urgent task.First, the article explain the general development of the Magnetotell-uric and its data processing ,and explain the method of the explores and the techniques of the earthquake explore , and discuss the basic principles of the pseudo - seismic interpretation;Deduced the formula under the 1D section model write out the calculation procedure of the pseudo - seismic , We computed the two-layer, three-layer and four-layer of 1D of the differ- rent model parameter.It is obvious that the pseudo - seismic interpretation can divide the line of the reflection and electricity layers,under the condition of lD,The inversion of the influence regulation of result from drawing up the earthquake method to commence in" tiny layer", inquiry into" tiny layer" to, with two layers of 1D, three" tiny layer" of different from four layers for model, pass to take thickness of layers, the inversion to compute the glint coefficient, tally up" tiny layer" of different thickness, to anti- play basic regulation of the result influence is: 1) the same model,with different thickness" tiny layer" parameter,which is anti- to play the not exhausted ho-mology of result;2) the " tiny layer" thickness was divided more thin, the inversion result wad more precious;3) " tiny layer" thickness is more thin, the inversion to compute time more long, the cost increase high;4) the first floor electricity layer divides the line to two" tiny layer" at least,
then can guarantee thus the inversion accuracy of result.The article argument that under the condition of lD,the earth elect-romagnetism measure and draw up the earthquake time section to explain the method and can divide the line to reflect the interface and electricity layers availably . At the same time , the " tiny layer" thickness to inversion the influence regulation study of compute the result, argument" tiny layer" thickness is one of the key techniques that the influence draws up not unique that the earthquake explains the solution, reasonably choice the " tiny layer" thickness and parameter is an accuracy and credibility, carry out the inversion of more prcious physics model.
本文首先概述了大地电磁测深的发展概况及其数据处理的方法技术,重点阐述了大地电磁测深和地震勘探法的相关技术,论述了拟地震解释法的基本原理;推导了一维断面模型下拟地震法的反演计算公式,编写出了计算拟地震反射系数的程序;论文计算了一维两层、三层和四层不同模型参数的反射系数,说明在一维水平均匀层状介质条件下,大地电磁测深拟地震时间剖面解释方法能有效地划分反射界面和电性层位。
论文又从拟地震法中“微层”入手,探讨“微层”对反演结果的影响规律,以一维两层、三层和四层为模型,通过取不同厚度“微层”,反演计算反射系数,总结了不同厚度“微层”,对反演结果影响的基本规律是:1、相同模型不同厚度“微层”参数,其反演结果不尽相同;2、“微层”厚度划分越细,反演的结果与实际越接近;3、“微层”厚度越细,反演计算时间越长,成本增高;4、第一层电性层至少划分为两个“微层”,这样才能保证反演结果的正确性。
论文通过计算不同模型参数的反射系数的变化规律,论证在一维水平均匀层状介质条件下,大地电磁测深拟地震时间剖面解释方法能有效地划分反射界面和电性层位。同时,论文又通过“微层”厚度对反演计算结果的影响规律探讨,论证了“微层”厚度是影响拟地震解释法解的非唯一性的关键技术之一,科学合理选择“微层”厚度参数是提高解的精度和可靠性,实现反演更接近真实的地球物理模型的基础。
The pseudo - seismic interpretation is the method of to draw up the earthquake to explain the method deeply according to the similar to flexible wave express the formality and the physics meanings in mathematics top certainly all have principle of electromagnetic wave, valid method go in the earthquake method to use to carry the electromagnetism method of a kind of electromagnetism explain the method. The pseudo - seismic interpretation , can divide the line to reflect the interface availably under the condition of 1D , compared with the normal regulations that it have its own characteristics , but the pseudo - seismic interpretation like other Earths physics methods all exist fault. Therefore, how contract and judge the fault and raise the accuracy and credibility of the solution, becoming a urgent task.First, the article explain the general development of the Magnetotell-uric and its data processing ,and explain the method of the explores and the techniques of the earthquake explore , and discuss the basic principles of the pseudo - seismic interpretation;Deduced the formula under the 1D section model write out the calculation procedure of the pseudo - seismic , We computed the two-layer, three-layer and four-layer of 1D of the differ- rent model parameter.It is obvious that the pseudo - seismic interpretation can divide the line of the reflection and electricity layers,under the condition of lD,The inversion of the influence regulation of result from drawing up the earthquake method to commence in" tiny layer", inquiry into" tiny layer" to, with two layers of 1D, three" tiny layer" of different from four layers for model, pass to take thickness of layers, the inversion to compute the glint coefficient, tally up" tiny layer" of different thickness, to anti- play basic regulation of the result influence is: 1) the same model,with different thickness" tiny layer" parameter,which is anti- to play the not exhausted ho-mology of result;2) the " tiny layer" thickness was divided more thin, the inversion result wad more precious;3) " tiny layer" thickness is more thin, the inversion to compute time more long, the cost increase high;4) the first floor electricity layer divides the line to two" tiny layer" at least,
then can guarantee thus the inversion accuracy of result.The article argument that under the condition of lD,the earth elect-romagnetism measure and draw up the earthquake time section to explain the method and can divide the line to reflect the interface and electricity layers availably . At the same time , the " tiny layer" thickness to inversion the influence regulation study of compute the result, argument" tiny layer" thickness is one of the key techniques that the influence draws up not unique that the earthquake explains the solution, reasonably choice the " tiny layer" thickness and parameter is an accuracy and credibility, carry out the inversion of more prcious physics model.
引文
[1] Cagniard L. Base theory of the magnetotelluric method of geophysical propecting. Geophysics, 1953,18 (2): 605～635
[2] F.W. Jones and D.J. Thomson, a discussion of the finite difference computer modeling of electrical conductivity structure, a reply to the by Williamson. Geophys.J.R. astr. SOC, 1974,37(3): 537～544
[3] 陈明生,严又生.二维水平电偶源极变频测深阻抗视电阻率的有限元正演计算.地球物理学报,1987,30(7):201～208
[4] M. Yamashita and P.G. Hallof. CSAMT case histories with a multi—channel CSAMT system and discussion of near-field data correction. Phoenix Geophysics Ltd, 1985
[5] 罗延钟,周玉林等.一种新的CSAMT资料近场校正方法.勘查地球物理勘查地球化学文集,1996,20(9):121～130
[6] Maxwell A. Meju. Joint. inversion of tem and distorted mt soundings:some effect practical consideration. Geophysics. 1996.61 (2): 56-65
[7] 吴小平,吴广耀等.二维最平模型的大地电磁快速反演。地球科学,1994,19(5):822～829
[8] A.G. Jones and R.W. Groom. strike-angle determination from the magnetotelluric impedance tensor in the presence of noise and local distortion: roatae at your peril. Geophys.J.Int, 1993,113 (12):524～534
[9] Xiaobo Li and L.B. pedsersen, controlled-source tensor magnetaotelluric responses of a layered earth with azimuthal nisotropy. Geophys. J. Int, 1992,111 (12): 91～103
[10] G. Fischer and W. Masero. rotational properties the magnetotelluric impedance tensor: the example of araguainha impact crater, brazil.Geophys. J. Int, 1994,119 (2): 548～560
[11] R.P. Singh and Yash Kant. sensitivity analysis of an over exponentially varying conductivity earth models. Geophys. J. Int, 1995,121 (7):111～116
[12] 何继善等编译.可控源音频大地电磁法.长沙:中南工业大学出版社,1990
[13] A.A.考夫曼,凯勒著.频率域和时间域电磁测深.北京:地质出版社,1987
[14] A.A.考夫曼,凯勒著.大地电磁测深.北京:地质出版社,1987
[15] 刘国栋,陈乐寿.大地电磁测深法研究.北京:地震出版社,1984
[16] 周虬.一种简易的一维大地电磁测深反演方法.石油地球物理勘探,1985 20(1):80～88
[17] 陈乐寿,王光锷等.一种大地电磁成像技术.地球物理学报,1993,36(2):337～346
[18] 师学明,王家映,张胜业,胡祥云.多尺度逐次逼近遗传算法反演大地电 磁资料.地球物理学报,2000,43(3):122～129
[19] A.T. Basokur, C. Kaya, E.U. Ulugergerli. direct interpretation of magnetotelluric sounding data based on the frequency-normalized impedance function, geophysical prospecting, 1997,45,21～37
[20] 王家映.Douglas Oldenburg,Shlomo Levy.大地电磁测深拟地震解释法.石油地球物理勘探,1985,7(20):66～79
[21] 吴广耀,叶兴茂.大地电磁二维波动方程深度偏移.电磁方法研究与勘探,1993,44～51
[22] Mrinals, Stoffa P L. Global Optimization Methods in Geophysical Inversion. Elsevier, 1995
[23] Arts E, Korst J. Simulated Annealing and Boltzmann Machines. John Welly & Sons, 1989
[24] Metropol, Rosenbluth et al. Equation of state calculations by fast computing machines. J Chem-Phys, 1953,21(20): 1087～1092
[25] Hedlin and constable. Occam, S inversion to generate smooth two-dimensional models from magnetotelluric data. Geophysics, 1990,2 (5): 1613～1624
[26] G. Kunetz. Processing and interpretation of magnetotelluric sounding. Geophysics, 1972,11 (7): 1005～1021
[27] S. Levy, D. Oldenberg and J. Wang. Subsurface imaging using magnetotelluric data. Geophysics, 1988,2 (3): 104～117
[28] S. Lee, G.A. McMechan and C.L. Aiken, Phase field imaging: the electromagnetic equivalent of seismic migration, Geophysics, 1987,5 (52) ,678～693
[29] V. SaSaki. Migration of magnetotelluric data by the phase-shift method. Geophysics propecting, 1989,1 (42): 177～18
[30] F.W. Jones and D.J. Thomson. a discussion of the finite difference computer modeling of electrical conductivity structure .Geophys. J. R. astr. SOC, 1974,37,537～544
[31] 陈明生,严又生.二维水平电偶源极变频测深阻抗视电阻率的有限元正演计算.地球物理学报,1987,30(8):201～208
[32] Maxwell A. Meju. Joint inversion of MT and distorted MT soundings: some effect practical consideration. Geophysics, 1996,61,56～65
[33] 吴小平,吴广耀等.二维最平模型的大地电磁快速反演.地球科学,1994,19(2):822～829
[34] M. Yamashita and P.G. Hallof. CSAMT case histories with a multichannel CSAMT system and discussion of near-field data correction. Phoenix Geophysics Ltd, 1985
[35] 罗延钟,周玉林等.一种新的CSAMT资料近场校正方法.勘查地球物理勘查地球化学文集,1996
[36] R.P. Singh and Yash Kant. sensitivity analysis of an over exponentially varying conductivity earth models. Geophys. J. Int, 1995,121(5):111～116
[37] G. Fischer and W. Masero. rotational properties the magnetotel- luric impedance tensor:the example of araguainha impact crater, brazil Geophys. J. Int, 1994,119 (7): 548～560
[38] A.G. Jones and R.W. Groom. strike-angle determination from the magnetotelluric impedance tensor in the presence of noise and local distortion: roatae at your peril. Geophys. J. Int, 1993,113 (9): 524～534
[39] Xiaobo Li and L.B. pedsersen. Controlled-source tensor magnetotelluric responses of a layered earth with azimuthal anisotropy. Geophys.J.Int, 1992,91～103
[40] 张贤达.非平稳信号分析与处理.北京:国防工业出版社,1998
[41] Trad and J.M. Travassos. Wavelet filtering of magnetotelluric data. Geophysics, 2000,65 (12): 482～491
[42] 师学明,王家映,张胜业,胡祥云.多尺度逐次逼近遗传算法反演大地电磁资料[J].地球物理学报,2000,43(6):122～129
[43] 李世雄,汪继文.信号的瞬时参数与正交小波基.地球物理学报,2000,43(11):97～103
[44] 徐义贤,王家映.基于连续小波变化的大地电磁信号谱估计方法.地球物理学报,2000,43(4):676～683
[45] T.A. Ridsdill smith and M.C. Dentith. The Wavelet transform in aeromagnetic processing. Geophysics, 1999,64 (3): 1003～1013
[46] P. Hornby, F. Boschetti and F.G. Horowize. Analysis of potential field data the wavelet domain. Geophys. J. Int, 1999,137,175～196
[47] M. Alexandrescu, D. Gibert. Detection of geomagnetic jerks using wavelet analysi S.J. Geophys. Res, 1995,100 (12): 12557～12572
[48] M. Fedi and T. Quarta Wavelet analysis for the regional-residual and local separation of potential field anomalies. Geophysical prospec ting, 1998,46 (8): 507～525
[49] V. Tarasov, E. Dubinin etal. Wavelet appl ication to the magnetic field turbulence in the upstream region of the martian bow shock. Earth Planets Space, 1998,50 (6): 699～708
[50] 何樵登.应用地球物理勘探教程-地震勘探.北京:地质出版社,1991
[51] 黄洪泽.折射波法探测断层的模拟试验.地球物理学报,1978,21(2):174～181
[52] 刘企英.利用地震信息进行油气预测.北京:石油工业出版社,1994,8
[53] 王彦春.神经网络及其在石油物探中的应用.[博士学位论文].成都:成都理工学院,1994
[54] 于德武.计算模糊相似优先比的FORTRAN程序.物探化探计算技术,1995,17(1):38～41
[55] 裴正林.小波理论及其在地震数据处理中的应用.地球物理学进展,2002,1(9):486～490
[56] 裴江云.地震波场延拓+菲涅尔体叠加方法及成像效果.中国科学院地北京:地质与地球物理研究所,2002,35～39
[57] 张建中.地震勘探初至波正反演及静校正方法研究.成都:成都理工学院,2001,26～31
[58] 杨勤勇,徐丽萍.地震勘探新技术.勘探地球物理进展,2002,5(1):25～ 30
[59] 徐颖,郑朝平.地震资料处理技术新进展.勘探地球物理进展,2003,(6):15～18
[60] SEG第68届年会论文概要.北京:石油工业出版社,1999
[61] SEG第69届年会论文概要.北京:石油工业出版社,2000
[62] SEG第70届年会论文概要.北京:石油工业出版社,2001
[63] Expanded Abstracts of SEG Seventy-First Annual Meeting. 2001
[64] 方伍宝.深度域成像技术的研究现状及发展趋势.石油物探信息,2000,15(3):11～13
[65] Gray S H. Seismic imaging.Geophysics, 2001,66(1): 15～17
[66] 黄中玉.多分量地震勘探的机遇与挑战.石油物探,2001,40(2):131～137
[67] 王家映.大地电磁拟地震解释法.石油地球物理勘探,1985
[68] 刘晓山,王家映.一种新的大地电磁反演方法—垂直时距曲线法.石油地球物理勘探,1987
[69] 席振铢,张宪润.武广铁路客运专线大地电磁探测报告.长沙:中南大学信息物理工程学院,2004
[70] 郭文波.瞬变电磁拟地震解释法研究.西安:西安工程学院,2000
[71] 李世华,杨有法.物探数据处理.北京:地质出版社,1995
[72] 方文藻,李予国,李貅.瞬变电磁测深法原理.西安:西北工业大学出版社,1993
[2] F.W. Jones and D.J. Thomson, a discussion of the finite difference computer modeling of electrical conductivity structure, a reply to the by Williamson. Geophys.J.R. astr. SOC, 1974,37(3): 537～544
[3] 陈明生,严又生.二维水平电偶源极变频测深阻抗视电阻率的有限元正演计算.地球物理学报,1987,30(7):201～208
[4] M. Yamashita and P.G. Hallof. CSAMT case histories with a multi—channel CSAMT system and discussion of near-field data correction. Phoenix Geophysics Ltd, 1985
[5] 罗延钟,周玉林等.一种新的CSAMT资料近场校正方法.勘查地球物理勘查地球化学文集,1996,20(9):121～130
[6] Maxwell A. Meju. Joint. inversion of tem and distorted mt soundings:some effect practical consideration. Geophysics. 1996.61 (2): 56-65
[7] 吴小平,吴广耀等.二维最平模型的大地电磁快速反演。地球科学,1994,19(5):822～829
[8] A.G. Jones and R.W. Groom. strike-angle determination from the magnetotelluric impedance tensor in the presence of noise and local distortion: roatae at your peril. Geophys.J.Int, 1993,113 (12):524～534
[9] Xiaobo Li and L.B. pedsersen, controlled-source tensor magnetaotelluric responses of a layered earth with azimuthal nisotropy. Geophys. J. Int, 1992,111 (12): 91～103
[10] G. Fischer and W. Masero. rotational properties the magnetotelluric impedance tensor: the example of araguainha impact crater, brazil.Geophys. J. Int, 1994,119 (2): 548～560
[11] R.P. Singh and Yash Kant. sensitivity analysis of an over exponentially varying conductivity earth models. Geophys. J. Int, 1995,121 (7):111～116
[12] 何继善等编译.可控源音频大地电磁法.长沙:中南工业大学出版社,1990
[13] A.A.考夫曼,凯勒著.频率域和时间域电磁测深.北京:地质出版社,1987
[14] A.A.考夫曼,凯勒著.大地电磁测深.北京:地质出版社,1987
[15] 刘国栋,陈乐寿.大地电磁测深法研究.北京:地震出版社,1984
[16] 周虬.一种简易的一维大地电磁测深反演方法.石油地球物理勘探,1985 20(1):80～88
[17] 陈乐寿,王光锷等.一种大地电磁成像技术.地球物理学报,1993,36(2):337～346
[18] 师学明,王家映,张胜业,胡祥云.多尺度逐次逼近遗传算法反演大地电 磁资料.地球物理学报,2000,43(3):122～129
[19] A.T. Basokur, C. Kaya, E.U. Ulugergerli. direct interpretation of magnetotelluric sounding data based on the frequency-normalized impedance function, geophysical prospecting, 1997,45,21～37
[20] 王家映.Douglas Oldenburg,Shlomo Levy.大地电磁测深拟地震解释法.石油地球物理勘探,1985,7(20):66～79
[21] 吴广耀,叶兴茂.大地电磁二维波动方程深度偏移.电磁方法研究与勘探,1993,44～51
[22] Mrinals, Stoffa P L. Global Optimization Methods in Geophysical Inversion. Elsevier, 1995
[23] Arts E, Korst J. Simulated Annealing and Boltzmann Machines. John Welly & Sons, 1989
[24] Metropol, Rosenbluth et al. Equation of state calculations by fast computing machines. J Chem-Phys, 1953,21(20): 1087～1092
[25] Hedlin and constable. Occam, S inversion to generate smooth two-dimensional models from magnetotelluric data. Geophysics, 1990,2 (5): 1613～1624
[26] G. Kunetz. Processing and interpretation of magnetotelluric sounding. Geophysics, 1972,11 (7): 1005～1021
[27] S. Levy, D. Oldenberg and J. Wang. Subsurface imaging using magnetotelluric data. Geophysics, 1988,2 (3): 104～117
[28] S. Lee, G.A. McMechan and C.L. Aiken, Phase field imaging: the electromagnetic equivalent of seismic migration, Geophysics, 1987,5 (52) ,678～693
[29] V. SaSaki. Migration of magnetotelluric data by the phase-shift method. Geophysics propecting, 1989,1 (42): 177～18
[30] F.W. Jones and D.J. Thomson. a discussion of the finite difference computer modeling of electrical conductivity structure .Geophys. J. R. astr. SOC, 1974,37,537～544
[31] 陈明生,严又生.二维水平电偶源极变频测深阻抗视电阻率的有限元正演计算.地球物理学报,1987,30(8):201～208
[32] Maxwell A. Meju. Joint inversion of MT and distorted MT soundings: some effect practical consideration. Geophysics, 1996,61,56～65
[33] 吴小平,吴广耀等.二维最平模型的大地电磁快速反演.地球科学,1994,19(2):822～829
[34] M. Yamashita and P.G. Hallof. CSAMT case histories with a multichannel CSAMT system and discussion of near-field data correction. Phoenix Geophysics Ltd, 1985
[35] 罗延钟,周玉林等.一种新的CSAMT资料近场校正方法.勘查地球物理勘查地球化学文集,1996
[36] R.P. Singh and Yash Kant. sensitivity analysis of an over exponentially varying conductivity earth models. Geophys. J. Int, 1995,121(5):111～116
[37] G. Fischer and W. Masero. rotational properties the magnetotel- luric impedance tensor:the example of araguainha impact crater, brazil Geophys. J. Int, 1994,119 (7): 548～560
[38] A.G. Jones and R.W. Groom. strike-angle determination from the magnetotelluric impedance tensor in the presence of noise and local distortion: roatae at your peril. Geophys. J. Int, 1993,113 (9): 524～534
[39] Xiaobo Li and L.B. pedsersen. Controlled-source tensor magnetotelluric responses of a layered earth with azimuthal anisotropy. Geophys.J.Int, 1992,91～103
[40] 张贤达.非平稳信号分析与处理.北京:国防工业出版社,1998
[41] Trad and J.M. Travassos. Wavelet filtering of magnetotelluric data. Geophysics, 2000,65 (12): 482～491
[42] 师学明,王家映,张胜业,胡祥云.多尺度逐次逼近遗传算法反演大地电磁资料[J].地球物理学报,2000,43(6):122～129
[43] 李世雄,汪继文.信号的瞬时参数与正交小波基.地球物理学报,2000,43(11):97～103
[44] 徐义贤,王家映.基于连续小波变化的大地电磁信号谱估计方法.地球物理学报,2000,43(4):676～683
[45] T.A. Ridsdill smith and M.C. Dentith. The Wavelet transform in aeromagnetic processing. Geophysics, 1999,64 (3): 1003～1013
[46] P. Hornby, F. Boschetti and F.G. Horowize. Analysis of potential field data the wavelet domain. Geophys. J. Int, 1999,137,175～196
[47] M. Alexandrescu, D. Gibert. Detection of geomagnetic jerks using wavelet analysi S.J. Geophys. Res, 1995,100 (12): 12557～12572
[48] M. Fedi and T. Quarta Wavelet analysis for the regional-residual and local separation of potential field anomalies. Geophysical prospec ting, 1998,46 (8): 507～525
[49] V. Tarasov, E. Dubinin etal. Wavelet appl ication to the magnetic field turbulence in the upstream region of the martian bow shock. Earth Planets Space, 1998,50 (6): 699～708
[50] 何樵登.应用地球物理勘探教程-地震勘探.北京:地质出版社,1991
[51] 黄洪泽.折射波法探测断层的模拟试验.地球物理学报,1978,21(2):174～181
[52] 刘企英.利用地震信息进行油气预测.北京:石油工业出版社,1994,8
[53] 王彦春.神经网络及其在石油物探中的应用.[博士学位论文].成都:成都理工学院,1994
[54] 于德武.计算模糊相似优先比的FORTRAN程序.物探化探计算技术,1995,17(1):38～41
[55] 裴正林.小波理论及其在地震数据处理中的应用.地球物理学进展,2002,1(9):486～490
[56] 裴江云.地震波场延拓+菲涅尔体叠加方法及成像效果.中国科学院地北京:地质与地球物理研究所,2002,35～39
[57] 张建中.地震勘探初至波正反演及静校正方法研究.成都:成都理工学院,2001,26～31
[58] 杨勤勇,徐丽萍.地震勘探新技术.勘探地球物理进展,2002,5(1):25～ 30
[59] 徐颖,郑朝平.地震资料处理技术新进展.勘探地球物理进展,2003,(6):15～18
[60] SEG第68届年会论文概要.北京:石油工业出版社,1999
[61] SEG第69届年会论文概要.北京:石油工业出版社,2000
[62] SEG第70届年会论文概要.北京:石油工业出版社,2001
[63] Expanded Abstracts of SEG Seventy-First Annual Meeting. 2001
[64] 方伍宝.深度域成像技术的研究现状及发展趋势.石油物探信息,2000,15(3):11～13
[65] Gray S H. Seismic imaging.Geophysics, 2001,66(1): 15～17
[66] 黄中玉.多分量地震勘探的机遇与挑战.石油物探,2001,40(2):131～137
[67] 王家映.大地电磁拟地震解释法.石油地球物理勘探,1985
[68] 刘晓山,王家映.一种新的大地电磁反演方法—垂直时距曲线法.石油地球物理勘探,1987
[69] 席振铢,张宪润.武广铁路客运专线大地电磁探测报告.长沙:中南大学信息物理工程学院,2004
[70] 郭文波.瞬变电磁拟地震解释法研究.西安:西安工程学院,2000
[71] 李世华,杨有法.物探数据处理.北京:地质出版社,1995
[72] 方文藻,李予国,李貅.瞬变电磁测深法原理.西安:西北工业大学出版社,1993