全球观测应力场的短波分量分析
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摘要
世界应力图(WSM,World Stress Map)计划的应力指标,目前已累积数据共计10 920个,这些应力指标代表了该地区最大水平主应力的实际观测方向;与此同时,可以假定全球各个板块的绝对运动方向表征了相应各板块的最大水平主应力方向的长波分量.根据应力场的叠加原理,得到由该地区局部构造运动等因素贡献的短波分量的相对大小和方向.将全球划分成2.5×2.5的基本单元,对每个单元的WSM数据进行加权统计分析,得到其平均应力观测取向,利用HS2-NUVEL1全球绝对板块运动模型计算应力场的长波分量;平均观测应力取向和长波分量取向之间的夹角,决定了相应短波分量相对于观测应力场的大小及其取向的范围,并反映了特定研究地区局部应力场对总应力场的贡献程度.本文的计算结果表明,全球板块的绝大部分地区及各板块的平均效果,长波分量与短波分量对观测应力场的贡献程度相当.对于某些大陆板块内部,局部构造活动对观测应力场的贡献起到重要作用,因而控制着地震的孕育与发生.
The 10 920 stress indicators collected so far by the WSM (World Stress Map) project represent the observed orientations of the maximum horizontal principal stress (sHmax) in a certain region. Assuming that the long-wave component of sHmax is expressed by the absolute direction of plate motions, we can get the relative orientation and the magnitude of the short-wave component resulted from the local tectonic process or other factors with vector analytical technique. The global surface was divided into basic element bins by 2.52.5 dimensions and the WSM indicators were statistically analyzed for each element by weight coefficient method in order to determine the mean orientation of the stress. We calculated the long-wave component of the global stress field using HS2-NUVEL1 model. The relative magnitude or the direction limitation of short-wave component, which reflect the local contribution to the observed stresses, was determined by the angle between the mean sHmax and the orientation of the long-wave component. The results of this paper show that the contribution of either the long-wave component or the short-wave component is approximately equal to most of the global plates on the basis of the mean effect of the observed stresses. For some of continental regions, the local active tectonics plays an important role in the observed stresses and controls the generation and occurrence of earthquakes.
The 10 920 stress indicators collected so far by the WSM (World Stress Map) project represent the observed orientations of the maximum horizontal principal stress (sHmax) in a certain region. Assuming that the long-wave component of sHmax is expressed by the absolute direction of plate motions, we can get the relative orientation and the magnitude of the short-wave component resulted from the local tectonic process or other factors with vector analytical technique. The global surface was divided into basic element bins by 2.52.5 dimensions and the WSM indicators were statistically analyzed for each element by weight coefficient method in order to determine the mean orientation of the stress. We calculated the long-wave component of the global stress field using HS2-NUVEL1 model. The relative magnitude or the direction limitation of short-wave component, which reflect the local contribution to the observed stresses, was determined by the angle between the mean sHmax and the orientation of the long-wave component. The results of this paper show that the contribution of either the long-wave component or the short-wave component is approximately equal to most of the global plates on the basis of the mean effect of the observed stresses. For some of continental regions, the local active tectonics plays an important role in the observed stresses and controls the generation and occurrence of earthquakes.
引文
魏东平,左如斌,濑野徹三．2001.全球观测应力场应力取向数据的加权统计分析[J].中国科学技术大学学报,31(1):50～56
魏东平.2000.软流层静压推力及其板块动力学意义[J].地质力学学报,6(1):4～14
DavisJ C.1986.Statistics andDataAnalysis inGeology[M].NewYork:JohnWiley&SonsPress,646
DeMetsC,GordonR G,ArgusD,et al.1990.Current plate motions[J].GeophysJ Int,101:425～478
GrippA E,GordonR G.1990.Current plate relative to the hotspots incorporating theNUVEL-1 global plate motion model[J].GeophyResLetters,17:1109～1112
MangaM,OConnellJ.1995.The tectosphere and postglacial rebound[J].GeophysResLett,22:1949～1952
MinsterJ B,JordanT H.1978.Present-day plate motion[J].J GeophysRes,83:5331～5354
MitrovicaJ X,DavisJ L,ShapiroI I.1994.A spectral formalism for computing three-dimensional deformations due to surface loads2.Present-day glacial isostatic adjustment[J].J GeophysRes,99:7075～7101
M黮lerB,ZocackM L,FuchsK,et al.1992.Regional patterns of stress inEurope[J].J GeophysRes,97:11783～11803
PacanovskyK M,RichardsonR M,DavisD M,et al.1999.Intraplate stresses and plate driving forces in thePhilippine sea plate[J].J GeophysRes,104(B1):1095～1110
RichardsonR M,RedingL M.1991.NorthAmerican plate dynamics[J].J GeophysRes,96:12201～12223
RichardsonR M.1992.Ridge forces, absolute plate motions, and the intraplate stress field[J].J GeophysRes,97:11739～11748
RichardsonR M,SolomonS C.1976.Intraplate stress as an indicator of plate tectonic driving forces[J].J GeophysRes,81:1847～1856
RichardsonR M,SolomonS C.1979.Tectonic stress in the plate[J].RevGeophysSpacePhys,17:981～1019
SabadiniR C,GiunchiC,GasperiniP,et al.1992.Plate motion and dragging of the upper mantle:Lateral variations of lithospheric thickness and their implications for intraplate deformation[J].GeophysResLett,19:749～752
StefanickM,JurdyD M.1992.Stress observations and driving force models for theSouthAmerican plate[J].J GeophysRes,97:11905～11913
WeiD P.1997.Pseudo-3-D SphericalModeling of theIntraplateStresses of theEurasianPlate:Implications toPlateDynamics[D].[学位论文].Tokyo:EarthquakeResearchInstitute ofUniversity ofTokyo,20～23
ZobackM L,ZobackM D.1989.Tectonic stress field of the conterminousUnitedStates[J].MenGeolSocAmer,172:523～539
ZobackM L,ZobackM D,AdamsJ,et al.1989.Global patterns of tectonic stress[J].Nature,341:291～298
ZobackM L.1992.First- and second-order patterns of stress in the lithosphere: theWorldStressMapProject[J].J GeophysRes,97:11703～11728
魏东平.2000.软流层静压推力及其板块动力学意义[J].地质力学学报,6(1):4～14
DavisJ C.1986.Statistics andDataAnalysis inGeology[M].NewYork:JohnWiley&SonsPress,646
DeMetsC,GordonR G,ArgusD,et al.1990.Current plate motions[J].GeophysJ Int,101:425～478
GrippA E,GordonR G.1990.Current plate relative to the hotspots incorporating theNUVEL-1 global plate motion model[J].GeophyResLetters,17:1109～1112
MangaM,OConnellJ.1995.The tectosphere and postglacial rebound[J].GeophysResLett,22:1949～1952
MinsterJ B,JordanT H.1978.Present-day plate motion[J].J GeophysRes,83:5331～5354
MitrovicaJ X,DavisJ L,ShapiroI I.1994.A spectral formalism for computing three-dimensional deformations due to surface loads2.Present-day glacial isostatic adjustment[J].J GeophysRes,99:7075～7101
M黮lerB,ZocackM L,FuchsK,et al.1992.Regional patterns of stress inEurope[J].J GeophysRes,97:11783～11803
PacanovskyK M,RichardsonR M,DavisD M,et al.1999.Intraplate stresses and plate driving forces in thePhilippine sea plate[J].J GeophysRes,104(B1):1095～1110
RichardsonR M,RedingL M.1991.NorthAmerican plate dynamics[J].J GeophysRes,96:12201～12223
RichardsonR M.1992.Ridge forces, absolute plate motions, and the intraplate stress field[J].J GeophysRes,97:11739～11748
RichardsonR M,SolomonS C.1976.Intraplate stress as an indicator of plate tectonic driving forces[J].J GeophysRes,81:1847～1856
RichardsonR M,SolomonS C.1979.Tectonic stress in the plate[J].RevGeophysSpacePhys,17:981～1019
SabadiniR C,GiunchiC,GasperiniP,et al.1992.Plate motion and dragging of the upper mantle:Lateral variations of lithospheric thickness and their implications for intraplate deformation[J].GeophysResLett,19:749～752
StefanickM,JurdyD M.1992.Stress observations and driving force models for theSouthAmerican plate[J].J GeophysRes,97:11905～11913
WeiD P.1997.Pseudo-3-D SphericalModeling of theIntraplateStresses of theEurasianPlate:Implications toPlateDynamics[D].[学位论文].Tokyo:EarthquakeResearchInstitute ofUniversity ofTokyo,20～23
ZobackM L,ZobackM D.1989.Tectonic stress field of the conterminousUnitedStates[J].MenGeolSocAmer,172:523～539
ZobackM L,ZobackM D,AdamsJ,et al.1989.Global patterns of tectonic stress[J].Nature,341:291～298
ZobackM L.1992.First- and second-order patterns of stress in the lithosphere: theWorldStressMapProject[J].J GeophysRes,97:11703～11728
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