垂向非均匀介质中首波特征分析
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摘要
利用合成理论地震图方法研究了存在高速层或低速层的地壳模型及壳-幔过渡带模型中首波等震相的动力学特征,指出首波的特征对于高速层的结构变化比较敏感.当高速层厚度与特征波长相比较小时,地震波的衍射现象明显,这种情况下高速层不能屏蔽在其下面一层的上界面传播的首波,且该首波震相的强度随高速层厚度或速度的增加而递减;当高速层厚度与特征波长相当时,高速层底面的反射波震相与首波震相到时接近,会因互相干涉而减弱;对于低速层,首波震相强度较弱且随低速层速度的减小而递减;在壳-幔间断处引入一定厚度和速度变化范围的过渡带,可以得到更加明显的视首波震相,强度随过渡带厚度或速度变化范围的增加而增大.
In this article, we analyze the dynamic characteristics of head wave in multi-layered half-space media models with high-velocity layer or low-velocity layer, and the model with a continuous transition-region between the crust and the mantle by using synthetic seismogram. It is concluded that the dynamic characteristics of head wave are sensitive to the thickness and velocity of the high-velocity layer. There is obvious diffraction phenomenon of seismic wave if the thickness of high-velocity layer is very small compared with the characteristic wavelength. In this case, the high-velocity layer cannot shield the head wave propagating along the upper interface of the media below it, and the amplitude of this head wave is proportional to the thickness or the velocity of wave propagation of the high-velocity layer. When the thickness of high-velocity layer is nearly identical to the characteristic wavelength of seismic wave, the wave phases reflected from the bottom of the high-velocity layer and the head wave phase may have very close arrival and weaken each other because of destructive interference. As to low-velocity layer, the amplitude of the head wave is weak and decreases with the velocity of this layer. It is also found that if a continuous transition-region between the crust and the mantle is introduced, we can get a strong apparent head wave phase in synthetic seismogram and the amplitude of this phase increases with the thickness or velocity gradient of the transitional region.
In this article, we analyze the dynamic characteristics of head wave in multi-layered half-space media models with high-velocity layer or low-velocity layer, and the model with a continuous transition-region between the crust and the mantle by using synthetic seismogram. It is concluded that the dynamic characteristics of head wave are sensitive to the thickness and velocity of the high-velocity layer. There is obvious diffraction phenomenon of seismic wave if the thickness of high-velocity layer is very small compared with the characteristic wavelength. In this case, the high-velocity layer cannot shield the head wave propagating along the upper interface of the media below it, and the amplitude of this head wave is proportional to the thickness or the velocity of wave propagation of the high-velocity layer. When the thickness of high-velocity layer is nearly identical to the characteristic wavelength of seismic wave, the wave phases reflected from the bottom of the high-velocity layer and the head wave phase may have very close arrival and weaken each other because of destructive interference. As to low-velocity layer, the amplitude of the head wave is weak and decreases with the velocity of this layer. It is also found that if a continuous transition-region between the crust and the mantle is introduced, we can get a strong apparent head wave phase in synthetic seismogram and the amplitude of this phase increases with the thickness or velocity gradient of the transitional region.
引文
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ChenX F.1999.Seismogram synthesis in multi-layered half-space.PartI.Theoretical formulation[J].EarthqResChina,13(2):150～174
ChenX F,QuanY L,JerryM H.1996.Seismogram synthesis for radially layered media using the generalized reflection/transmission coefficients method:Theory and applications to a coustic logging[J].Geophysics,61(4):1150～1159
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FuchsK,MüllerG.1971.Computation of synthetic seismograms with reflectivity method and comparison with observations[J].GeophysJ R astrSoc,23:417～433
HelmbergerD V.1974.Generalized ray theory for shear dislocations[J].BullSeismSocAmer,64:45～64
KennettB L N.1983.SeismicWavePropagation inStratifiedMedia[M].NewYork:CambridgeUniversityPress,1～5
LucoJ E,ApselR J.1983.On theGreens function for a layered half-space[J].BullSeismSocAmer,73:909～951
YaoZ X,HarkriderD G.1983.A generalized reflection-transmission coefficient matrix and discrete wavenumber method for synthetic seismograms[J].BullSeismSocAmer,73:1685～1699
ChenX F.1993.A systematic and efficient method of computing normal models for multilayered half-space[J].GeophysJ Int,115(2):391～409
ChenX F.1999.Seismogram synthesis in multi-layered half-space.PartI.Theoretical formulation[J].EarthqResChina,13(2):150～174
ChenX F,QuanY L,JerryM H.1996.Seismogram synthesis for radially layered media using the generalized reflection/transmission coefficients method:Theory and applications to a coustic logging[J].Geophysics,61(4):1150～1159
ChenX F,ZhangH M.2001.An efficient method for computingGreens functions for a layered half-space at large epicentral distances[J].BullSeismSocAmer,91:858～869
FuchsK,MüllerG.1971.Computation of synthetic seismograms with reflectivity method and comparison with observations[J].GeophysJ R astrSoc,23:417～433
HelmbergerD V.1974.Generalized ray theory for shear dislocations[J].BullSeismSocAmer,64:45～64
KennettB L N.1983.SeismicWavePropagation inStratifiedMedia[M].NewYork:CambridgeUniversityPress,1～5
LucoJ E,ApselR J.1983.On theGreens function for a layered half-space[J].BullSeismSocAmer,73:909～951
YaoZ X,HarkriderD G.1983.A generalized reflection-transmission coefficient matrix and discrete wavenumber method for synthetic seismograms[J].BullSeismSocAmer,73:1685～1699
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