西藏桑日县沃卡地堑的第四纪正断层活动及其机制探讨
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摘要
遥感解译和地表调查结果发现,西藏桑日县的沃卡盆地构成了藏南近南北向裂谷带中最东端的错那-沃卡裂谷的北段,它是在该区近东西向的逆冲构造带停止活动之后,上地壳沿N108±1°E方向发生区域性的伸展变形所形成的第四纪活动明显的地堑式断陷盆地。晚第四纪期间,控制该盆地发育的主边界断裂带为整体呈北北东走向、倾向西侧、长50～60km的盆地东缘正断层。该断裂带也是1915年桑日M7.0级地震的控震断裂。断裂活动速率的估算结果表明,该断裂带MIS6以来的垂直活动速率介于0.4～0.9mm/a之间,末次冰期盛冰期以来断裂平均活动速率最合理的估计值为1.2±0.3mm/a。Q3晚期以来活动速率的明显增加可能标志着该断裂带全新世进入了地震丛集期。
The Oiga graben,belonging to the northern section of the NNE trending Cona-Oiga(or Cona-Sangri)rift zone which is the only rift located at the east of the Yadong-Gulu rift zone in southern Tibet,is a N18°E trending basin located around 92°15' E and between 29°10'N and 29°40'N,and cutting across the eastern Gangdese batholith zone at the north of the Yarlung Tsangpo fault(or Great counter thrust fault).It is about 50 km long and widens from 3～5 km in the south to 15～18 km in the north.Four sets of tills and fluvioglacial deposits are found in the basin,which are corresponding to the so-called Nyanyxungla Ice Age,Jilongshi Ice Age,Ronbushi Ice Age and Holocene glaciations respectively from oldest to youngest.The Thermal Luminescence(TL)age results associated with the deposits show that the first(or the oldest)tills formed before marine isotope stage(MIS)6(about 200～140 ka BP),the second set of tills formed during MIS6,the third and fourth moraines formed during the last Glacial maximum(about 28～15ka BP)and Holocene glaciations respectively.The graben is limited to the east and west by two N18±1°E-trending boundary faults of opposite dips about 50～60 km long and indicates that the extension direction is N108±1°E in the region.The field survey shows that the eastern margin fault of the Oiga basin,a west dipping normal fault,is the master boundary fault of the graben.It had been active from Quaternary or before that to Holocene,and is the seismogenic fault of 1915 M7.0 Sangri earthquake.In this region,it offset the Gangdese batholith zone,containing Jurassic-Cretaceous sedimentary rocks,early Tertiary volcanic sediment and late Cretaceous-early Tertiary granites,and is limited between the Great Counter fault in the south and the Modro Gongkar-Kongpo Gyamda fault in the north.The master boundary normal fault offset late Quaternary deposits showing obvious activity during the late Pleistocene and Holocene.Based on measure of fault scarp offset moraine platform and fluviaoglacial terraces,the displacements are 50～90 m,24.0±1.5 m,16.0±1.0 m or 13.7±0.5 m and 3.7±0.4 m since MIS6,24～18 ka BP,15～11 ka BP and middle-late Holocene respectively.Given such displacement of fault and ages of tills filling,the most probably values of throw rates on differential time scale are deduced.The Late Quaternary throw rates are limited between 0.4～0.9 mm/a,with the most probably value being 0.7±0.2 mm/a,and the throw rate is about 1.2±0.3 mm/a since MIS2 and during the Holocene.The Late Quaternary throw rates maybe constrain the uniform long-term slip rate along the eastern margin fault of the Oiga graben.The obviously increasing of the throw rate during the Holocene is most probably resulted from earthquake cluster in the Holocene.The new observation on the Oiga graben shows that the development of trends of the grabens or rifts is strictly limited in southern Tibet.The new long-term and short-term slip rates from the Oiga graben are also distinctly similar to the throw rate of inferred for normal faults bounding the west margin fault of Damxung-Yangbajain in the northern section of the Yadong-Gulu graben system.The strict geometry,pronounced similar and consistent on the active magnitude and trend of faults and grabens in southern Tibet suggests that the normal faulting in southern Tibet did not result from the mechanisms controlled largely by local processes,including oroclinal bending of the Himalaya orogen,right-laterally oblique convergence of the India continental lithosphere,right-lateral motion along the Karakorum-Jiali Fault Zone,a change in boundary conditions along the eastern margin of Asia,topographic collapse of an overthickened crust or advective removal of thickened Tibetan mantle lithosphere,and radial spreading of the Himalayan arc on the India plate.The most probably interpretation is that the uniform extension controlled by regional processes resulted from lower crust lateral flow in south Tibet or longitudinal extension resulted from lower crustal extension normal orogen.
The Oiga graben,belonging to the northern section of the NNE trending Cona-Oiga(or Cona-Sangri)rift zone which is the only rift located at the east of the Yadong-Gulu rift zone in southern Tibet,is a N18°E trending basin located around 92°15' E and between 29°10'N and 29°40'N,and cutting across the eastern Gangdese batholith zone at the north of the Yarlung Tsangpo fault(or Great counter thrust fault).It is about 50 km long and widens from 3～5 km in the south to 15～18 km in the north.Four sets of tills and fluvioglacial deposits are found in the basin,which are corresponding to the so-called Nyanyxungla Ice Age,Jilongshi Ice Age,Ronbushi Ice Age and Holocene glaciations respectively from oldest to youngest.The Thermal Luminescence(TL)age results associated with the deposits show that the first(or the oldest)tills formed before marine isotope stage(MIS)6(about 200～140 ka BP),the second set of tills formed during MIS6,the third and fourth moraines formed during the last Glacial maximum(about 28～15ka BP)and Holocene glaciations respectively.The graben is limited to the east and west by two N18±1°E-trending boundary faults of opposite dips about 50～60 km long and indicates that the extension direction is N108±1°E in the region.The field survey shows that the eastern margin fault of the Oiga basin,a west dipping normal fault,is the master boundary fault of the graben.It had been active from Quaternary or before that to Holocene,and is the seismogenic fault of 1915 M7.0 Sangri earthquake.In this region,it offset the Gangdese batholith zone,containing Jurassic-Cretaceous sedimentary rocks,early Tertiary volcanic sediment and late Cretaceous-early Tertiary granites,and is limited between the Great Counter fault in the south and the Modro Gongkar-Kongpo Gyamda fault in the north.The master boundary normal fault offset late Quaternary deposits showing obvious activity during the late Pleistocene and Holocene.Based on measure of fault scarp offset moraine platform and fluviaoglacial terraces,the displacements are 50～90 m,24.0±1.5 m,16.0±1.0 m or 13.7±0.5 m and 3.7±0.4 m since MIS6,24～18 ka BP,15～11 ka BP and middle-late Holocene respectively.Given such displacement of fault and ages of tills filling,the most probably values of throw rates on differential time scale are deduced.The Late Quaternary throw rates are limited between 0.4～0.9 mm/a,with the most probably value being 0.7±0.2 mm/a,and the throw rate is about 1.2±0.3 mm/a since MIS2 and during the Holocene.The Late Quaternary throw rates maybe constrain the uniform long-term slip rate along the eastern margin fault of the Oiga graben.The obviously increasing of the throw rate during the Holocene is most probably resulted from earthquake cluster in the Holocene.The new observation on the Oiga graben shows that the development of trends of the grabens or rifts is strictly limited in southern Tibet.The new long-term and short-term slip rates from the Oiga graben are also distinctly similar to the throw rate of inferred for normal faults bounding the west margin fault of Damxung-Yangbajain in the northern section of the Yadong-Gulu graben system.The strict geometry,pronounced similar and consistent on the active magnitude and trend of faults and grabens in southern Tibet suggests that the normal faulting in southern Tibet did not result from the mechanisms controlled largely by local processes,including oroclinal bending of the Himalaya orogen,right-laterally oblique convergence of the India continental lithosphere,right-lateral motion along the Karakorum-Jiali Fault Zone,a change in boundary conditions along the eastern margin of Asia,topographic collapse of an overthickened crust or advective removal of thickened Tibetan mantle lithosphere,and radial spreading of the Himalayan arc on the India plate.The most probably interpretation is that the uniform extension controlled by regional processes resulted from lower crust lateral flow in south Tibet or longitudinal extension resulted from lower crustal extension normal orogen.
引文
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韩同林.1986,试论西藏活动构造带及其对地震的控制作用.地质学报,60(4):332～338.
韩同林.1987.西藏活动构造.地质专报5(4).北京:地质出版社.
李吉均,文世宣,张青松,等.1979.青藏高原隆升的时代、幅度和形式探讨.中国科学(B辑),9(6):608～616.
吴章明.1992.对《西藏活动构造》一书中有关问题的讨论.地质论评,38(2):194～196.
吴中海,赵希涛,吴珍汉,等.2004a.西藏纳木错及邻区全新世气候与环境变化的地质记录.冰川冻土,26(3):275～283.
吴中海,吴珍汉,胡道功,等.2006.青藏铁路唐古拉山—拉萨段全新世控震断裂研究.地质通报,25(12):1387～1401.
西藏自治区科学技术委员会.1982.西藏地震史料汇编.拉萨:西藏人民出版社.
姚檀栋,Thompson L G,施雅风,等.1997.古里雅冰芯中末次间冰期以来气候变化记录研究.中国科学(D辑),27(5):447～452
钟大赉,丁林.1996.青藏高原的隆起过程及其机制探讨.中国科学(D辑),26(4):289～295.
中国科学院青藏高原综合科学考察队(李炳元、王富葆,张青松等).1983.西藏第四纪地质.北京:科学出版社.
Armijo R,Tapponier P,Mercier J L.1986.Quaternary extensionin southern Tibet:Field observations and tectonic implications.Journal of Geophysical Research,91:13803～13872.
Armijo R,Tapponnier P,Han T.1989.Late Cenozoic right-lateralstrike-slip faulting in southern Tibet.Journal of GeophysicalResearch,94:2787～2838.
Barnard P,Owen L A,Finkel R C.2006.Quaternary fans andterraces in the Khumbu Himal south of Mount Everest:theircharacteristics,age and formation.Journal of the GeologicalSociety,163:383～399.
Bendick R,Bilham R.2001.How perfect is the Himalayan arc?Geology,29:791～794.
Bond G,Broecker W,Johnsen S,et al.1993.Correlations Betweenclimate records from North Antarctic sediments and GreenlandIce.Nature,365:143～147.
Coleman M,Hodges K.1995.Evidence for Tibetan plateau upliftbefore14Myr ago from a new minimum age for east-westextension.Nature,374:49～52.
Comprehensive Scientific Expedition Group(Li Bingyuan,WangFubao,Zhang Qingsong,et al.).1983.Quaternary GeologyinXizang.Beijing:Science Press(in Chinese with Englishabstract).
Dewey J F,Shackleton R M,Chang Chengfa,et al.1988.Thetectonic evolution of the Tibetan Plateau.PhilosophicalTransaction of Royal Society of London,Series A,327:379～413.
England P,Houseman G.1989.Extension during continentalconvergence,with application to the Tibetan Plateau.Journalof Geophysical Research,94:17561～17569.
Hancock G S,Anderson R S,Chadwick O A,et al.1999.Datingfluvial terraces with10Be and26Al profile:application to theWind River,Wyoming.Geomorphology,27:41～60.
Hancock G S,Anderson R S.2002.Numerical modeling of fluvialstrath-terrace formation in response to oscillating climate.Geological Society of America Bulletin,114(9):1131～1142.
Han Tonglin.1986.Active tectonic belts in Tibet and their controlon earthquakes.Acta Geology Sinica,60(4):23～30.
Han Tonglin.1987.The active tectonic in Xizang(Tibet).Geological Memoirs,Series5(4).Beijing:GeologicalPublishing House(in Chinese with English abstract).
Hargreaves J C,Abe-Ouchi A.2003.Timing of ice-age terminationsdetermined by wavelet methods.Paleoceanography,18(2),1035,doi:10.1029/2002PA000825.
Harrison T M,Copeland P,Kidd W S F,et al.1992.RaisingTibet.Science,225:1663～1670.
Hetzel R S,Niedermann M,Tao,et al.2006.Climatic versustectonic control on river incision at the margin of NE Tibet:10Be exposure dating of river terraces at the mountain front ofthe Qilian Shan.Journal of Geophysical Research,111,F03012,doi:10.1029.
Kapp P,Guynn J H.2004.Indian punch rifts Tibet.Geology,32(11):993～996.
Klootwijk C T,Conaghan P J,Powell C M.1985.The Himalayanarc:large-scale continental subduction,oroclinal bending andback-arc spreading.Earth and Planetary Science Letters,75:167～183.
Le K,Lee J,Owen L A,et al.2007.Late Quaternary slip ratesalong the Sierra Nevada frontal fault zone,California:Slippartitioning across the the western margin of the easternCalifornia Shear Zone-Basin and Range Province.GeologicalSociety of America Bulletin,119:240～256.
Li Jijun,Wen Shixuan,Zhang Qingsong,et al.1979.A discussionon the period,amplitude and type of the uplift of the Qinghai-Xizang Plateau.Scientia Sinica,22(11):1314～1328(inEnglish).
Masek J G,Isacks B L,Fielding EJ,et al.1994.Rift-flank uplift inTibet:Evidence for a viscous lower crust.Tectonics,13:659～667.
McCaffrey R,Nabelek J.1998.Role of oblique convergence in theactive deformation of the Himalayas and southern Tibetplateau.Geology,26(8):691～694.
Mercier J L,Armijo R,Tapponier P,et al.1987.Change fromlateTertiary compression to Quaternary extensionin southern Tibetduring India-Asia collision.Tectonics,6(3):275～304.
Molnar P,Tapponnier P.1978.Active tectonics of Tibet.Journalof Geophysical Research,83:5361～5375.
Molnar P,England P,Martinod J.1993.Mantle dynamics,upliftof the Tibet plateau,and the Indian monsoon.Review ofGeophysics.31:357～396.
Ni J,York J E.1978.Late Cenozoic tectonics of the Tibetanplateau.Journal of Geophysical Research,83(B11):5377～5384.
Owen L A,Finkel R C,Caffee M W,et al.2002.Timing ofmultiple glaciations during the Late Quaternary in the HunzaValley,Karakoram Mountains,Northern Pakistan:defined bycosmogenic radionuclide dating of moraines.Geological Societyof America Bulletin,114:593～604.
Pan Baotian,Burbank D.2003.A900k.y.record of strathterraceformation during glacial-interglacial transitions in northwestChina.Geology,31(11):957～960.
Rothery D A,Drury S A.1984.The neotectonics of the Tibetanplateau.Tectonics,3(1):19～26.
Royden L H,Burchfiel C,King R W,et al.1997.Surfacedeformation and lower crustal flowin eastern Tibet.Science,276:788～790.
Science and Technology Committee of the Tibetan AutonomousRegion.1982.Records of Historical Earthquakes of Tibet.Lhasa:People's Press of the Tibet(in Chinese).
Seeber L,Pecher A.1998.Strain partitioning along the Himalayaarc and the Nanga Parbat antiform.Geology,26:791～794.
Starkel L.2003.Climatically controlled terraces in upliftingmountain areas.Quaternary Science Reviews,22:2189～2198.
Wallace R E.1987.Grouping and migration of surface faulting andvariation in slip rates on faults in the Great Basin province.Bull.Seism.Soc.Am.,77:868～877.
Wu Zhangming.1992.Discussion on some problems in the book-《The active tectonic in Xizang(Tibet)》.Geological Review,38(2):194～196(in Chinese with English abstract).
Wu Zhonghai,Zhao Xitao,Wu Zhenhan,et al.2004a.Geologicalrecords of climate and environment changes duringthe Holocenein the Nam Colake andits adjacent areas.Journal of Glaciologyand Geocryology,26(3):275～283(in Chinese with Englishabstract).
Wu Zhonghai,Zhao Xitao,Wu Zhenhan,et al.2004b.Quaternarygeology and faulting in the Damxung-Yangbajain basin.ActaGeology Sinica,78(1):273～282.
Wu Zhonghai,Wu Zhenhan,Hu Daogong,et al.2006.Holoceneseismogenic faults along the Tanggula-Lhasa section of theQinghai-Tibet rail way,China.Geological Bulletin of China,25(12):1387～1401(in Chinese with English abstract).
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Yin A.2000.Mode of Cenozoic east-west extension in Tibetsuggesting a common origin of riftsin Asia duringthe Indo-Asiacollision.Journal of Geophysical Research,105(B9):21745～21759.
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[2]陕西省地质矿产局区域地质调查大队三分队.1994.西藏加查幅1∶20万区域地质图.
韩同林.1986,试论西藏活动构造带及其对地震的控制作用.地质学报,60(4):332～338.
韩同林.1987.西藏活动构造.地质专报5(4).北京:地质出版社.
李吉均,文世宣,张青松,等.1979.青藏高原隆升的时代、幅度和形式探讨.中国科学(B辑),9(6):608～616.
吴章明.1992.对《西藏活动构造》一书中有关问题的讨论.地质论评,38(2):194～196.
吴中海,赵希涛,吴珍汉,等.2004a.西藏纳木错及邻区全新世气候与环境变化的地质记录.冰川冻土,26(3):275～283.
吴中海,吴珍汉,胡道功,等.2006.青藏铁路唐古拉山—拉萨段全新世控震断裂研究.地质通报,25(12):1387～1401.
西藏自治区科学技术委员会.1982.西藏地震史料汇编.拉萨:西藏人民出版社.
姚檀栋,Thompson L G,施雅风,等.1997.古里雅冰芯中末次间冰期以来气候变化记录研究.中国科学(D辑),27(5):447～452
钟大赉,丁林.1996.青藏高原的隆起过程及其机制探讨.中国科学(D辑),26(4):289～295.
中国科学院青藏高原综合科学考察队(李炳元、王富葆,张青松等).1983.西藏第四纪地质.北京:科学出版社.
Armijo R,Tapponier P,Mercier J L.1986.Quaternary extensionin southern Tibet:Field observations and tectonic implications.Journal of Geophysical Research,91:13803～13872.
Armijo R,Tapponnier P,Han T.1989.Late Cenozoic right-lateralstrike-slip faulting in southern Tibet.Journal of GeophysicalResearch,94:2787～2838.
Barnard P,Owen L A,Finkel R C.2006.Quaternary fans andterraces in the Khumbu Himal south of Mount Everest:theircharacteristics,age and formation.Journal of the GeologicalSociety,163:383～399.
Bendick R,Bilham R.2001.How perfect is the Himalayan arc?Geology,29:791～794.
Bond G,Broecker W,Johnsen S,et al.1993.Correlations Betweenclimate records from North Antarctic sediments and GreenlandIce.Nature,365:143～147.
Coleman M,Hodges K.1995.Evidence for Tibetan plateau upliftbefore14Myr ago from a new minimum age for east-westextension.Nature,374:49～52.
Comprehensive Scientific Expedition Group(Li Bingyuan,WangFubao,Zhang Qingsong,et al.).1983.Quaternary GeologyinXizang.Beijing:Science Press(in Chinese with Englishabstract).
Dewey J F,Shackleton R M,Chang Chengfa,et al.1988.Thetectonic evolution of the Tibetan Plateau.PhilosophicalTransaction of Royal Society of London,Series A,327:379～413.
England P,Houseman G.1989.Extension during continentalconvergence,with application to the Tibetan Plateau.Journalof Geophysical Research,94:17561～17569.
Hancock G S,Anderson R S,Chadwick O A,et al.1999.Datingfluvial terraces with10Be and26Al profile:application to theWind River,Wyoming.Geomorphology,27:41～60.
Hancock G S,Anderson R S.2002.Numerical modeling of fluvialstrath-terrace formation in response to oscillating climate.Geological Society of America Bulletin,114(9):1131～1142.
Han Tonglin.1986.Active tectonic belts in Tibet and their controlon earthquakes.Acta Geology Sinica,60(4):23～30.
Han Tonglin.1987.The active tectonic in Xizang(Tibet).Geological Memoirs,Series5(4).Beijing:GeologicalPublishing House(in Chinese with English abstract).
Hargreaves J C,Abe-Ouchi A.2003.Timing of ice-age terminationsdetermined by wavelet methods.Paleoceanography,18(2),1035,doi:10.1029/2002PA000825.
Harrison T M,Copeland P,Kidd W S F,et al.1992.RaisingTibet.Science,225:1663～1670.
Hetzel R S,Niedermann M,Tao,et al.2006.Climatic versustectonic control on river incision at the margin of NE Tibet:10Be exposure dating of river terraces at the mountain front ofthe Qilian Shan.Journal of Geophysical Research,111,F03012,doi:10.1029.
Kapp P,Guynn J H.2004.Indian punch rifts Tibet.Geology,32(11):993～996.
Klootwijk C T,Conaghan P J,Powell C M.1985.The Himalayanarc:large-scale continental subduction,oroclinal bending andback-arc spreading.Earth and Planetary Science Letters,75:167～183.
Le K,Lee J,Owen L A,et al.2007.Late Quaternary slip ratesalong the Sierra Nevada frontal fault zone,California:Slippartitioning across the the western margin of the easternCalifornia Shear Zone-Basin and Range Province.GeologicalSociety of America Bulletin,119:240～256.
Li Jijun,Wen Shixuan,Zhang Qingsong,et al.1979.A discussionon the period,amplitude and type of the uplift of the Qinghai-Xizang Plateau.Scientia Sinica,22(11):1314～1328(inEnglish).
Masek J G,Isacks B L,Fielding EJ,et al.1994.Rift-flank uplift inTibet:Evidence for a viscous lower crust.Tectonics,13:659～667.
McCaffrey R,Nabelek J.1998.Role of oblique convergence in theactive deformation of the Himalayas and southern Tibetplateau.Geology,26(8):691～694.
Mercier J L,Armijo R,Tapponier P,et al.1987.Change fromlateTertiary compression to Quaternary extensionin southern Tibetduring India-Asia collision.Tectonics,6(3):275～304.
Molnar P,Tapponnier P.1978.Active tectonics of Tibet.Journalof Geophysical Research,83:5361～5375.
Molnar P,England P,Martinod J.1993.Mantle dynamics,upliftof the Tibet plateau,and the Indian monsoon.Review ofGeophysics.31:357～396.
Ni J,York J E.1978.Late Cenozoic tectonics of the Tibetanplateau.Journal of Geophysical Research,83(B11):5377～5384.
Owen L A,Finkel R C,Caffee M W,et al.2002.Timing ofmultiple glaciations during the Late Quaternary in the HunzaValley,Karakoram Mountains,Northern Pakistan:defined bycosmogenic radionuclide dating of moraines.Geological Societyof America Bulletin,114:593～604.
Pan Baotian,Burbank D.2003.A900k.y.record of strathterraceformation during glacial-interglacial transitions in northwestChina.Geology,31(11):957～960.
Rothery D A,Drury S A.1984.The neotectonics of the Tibetanplateau.Tectonics,3(1):19～26.
Royden L H,Burchfiel C,King R W,et al.1997.Surfacedeformation and lower crustal flowin eastern Tibet.Science,276:788～790.
Science and Technology Committee of the Tibetan AutonomousRegion.1982.Records of Historical Earthquakes of Tibet.Lhasa:People's Press of the Tibet(in Chinese).
Seeber L,Pecher A.1998.Strain partitioning along the Himalayaarc and the Nanga Parbat antiform.Geology,26:791～794.
Starkel L.2003.Climatically controlled terraces in upliftingmountain areas.Quaternary Science Reviews,22:2189～2198.
Wallace R E.1987.Grouping and migration of surface faulting andvariation in slip rates on faults in the Great Basin province.Bull.Seism.Soc.Am.,77:868～877.
Wu Zhangming.1992.Discussion on some problems in the book-《The active tectonic in Xizang(Tibet)》.Geological Review,38(2):194～196(in Chinese with English abstract).
Wu Zhonghai,Zhao Xitao,Wu Zhenhan,et al.2004a.Geologicalrecords of climate and environment changes duringthe Holocenein the Nam Colake andits adjacent areas.Journal of Glaciologyand Geocryology,26(3):275～283(in Chinese with Englishabstract).
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