青藏高原中部温泉盆地西缘的晚新生代正断层作用
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摘要
在青藏高原中部的温泉盆地西侧发育了1条倾向东的强烈活动的近SN正断层——温泉盆地西缘断裂。它是在印度板块与欧亚板块强烈碰撞的背景下,青藏高原中北部地区自晚新生代以来发生近EW向伸展变形的产物。晚新生代以来,该断裂上的最大垂直错动量不会<21km,错动中生代褶皱地层所暗示的最大垂直位移量为(60±22)km。第四纪期间,该断裂发生了多期活动,形成了山前的多套断层三角面和多级断层陡坎地貌。根据断裂垂直错动晚第四纪期间不同时代的地层和地貌体所形成的断层崖高度估算,其晚第四纪以来的最大活动速率不超过12mm/a,平均活动速率为045mm/a。初步的探槽分析表明,晚更新世末期以来沿该断裂至少发生了3次震级不同的古地震事件。综合该断裂的全新世活动特点推断,它是在未来具有较大可能发生6～7级地震的一条重要控震断裂。
The north south trending Wenquan graben is located to the north of Tanggula Mountains in central Qinghai Tibet Plateau, having a length of about 40km and a width of 8～12km. The graben is filled with Quaternary moraine, fluvioglacial deposits and alluvia. An east dipping boundary normal fault of about 45km length is developed along the western margin of the graben, where the relief is dramatically varied. The fault offsets vertically the bedrock, alluvial fan, river terraces and travertine platform. On the upthrown side of the fault, there are 4 prominent fault facets, which are ～600m, ～400m, ～200m, and ～80m above the surface of piedmont plain, respectively. At the base of fault facets, sustained faulting has given rise to the formation of east facing fault scarps and surface ruptures that cut the terraces, alluvial fans and travertine platform. Leveling survey and in situ measurement with tape measure show that the 6 sets of fault scarps are about 0 3～0.6m, 4～5m, 8±1m, 15±3m, 24±4m and 45±5m in height, respectively, and that the higher the scarp, the older the strata cut by the scarp. Among them, the 0.3～0.6m high fault scarp might be associated with M S 6～7 earthquake of middle late Holocene, the 4～5m and 8±1m fault scarps offset separately the terraces Ⅰ and Ⅱ, while the 15±3m, 24±4m and 45±5m high fault scarps offset separately the terrace Ⅲ, Ⅳ, Ⅴ and travertine platform. U series dating results indicate that the fault scarp that offsets the terracesⅠand Ⅱ was formed 11～7ka BP, the scarp that offsets the terraces Ⅲ was formed 21～25ka BP, and the scarps that offset the terrace Ⅳ and Ⅴ and the correlated travertine platform were formed 45 2～53 6ka BP and 103～127ka BP, respectively. The 80～200m high scarps might be formed since 324～521ka BP. Moreover, the dating results suggest also that the average vertical slip rate along the normal fault on the western side of the Wenquan graben is 0.45mm/a with the maximum value of less than 1.2mm/a. The relief across the normal fault indicates that the minimum cumulative displacement on the fault is about 2.1km. The maximum cumulative throws on the fault is about 8.2km. The trenching across the fault revealed that at least 3 paleoseismic events have occurred along the fault since late Pleistocene. The magnitude of those events can be estimated to be M S 6～7 and the approximate recurrence interval to be from about 400 to 3000yr. The slip rate on normal fault from Wenquan graben implies that the east west extension rate absorbed by a single graben in central Tibet is significantly lower than that of the grabens in southern Tibet, but this does not imply that the east west extension rate in central Tibet must be significantly lower than that in southern Tibet. This is because that the east west extension in central Tibet might be accommodated by a larger number of normal and strike slip faults distributed in this area. On the basis of the total cumulative throws and the average vertical slip rate on the fault, it is inferred that the initiation time of the normal faulting to be at about 18 2～1 8Ma BP. The broad similarities in the magnitude of slip, the direction of extension and the initiation time of normal faulting in both central and southern Qinghai Tibet Pateau imply that the east west extension within the Qinghai Tibet Plateau has occurred synchronously, and that the crustal thickness in central and southern Tibet Plateau has reached its maximum value since Miocene, while the whole Plateau has reached its present elevation.
The north south trending Wenquan graben is located to the north of Tanggula Mountains in central Qinghai Tibet Plateau, having a length of about 40km and a width of 8～12km. The graben is filled with Quaternary moraine, fluvioglacial deposits and alluvia. An east dipping boundary normal fault of about 45km length is developed along the western margin of the graben, where the relief is dramatically varied. The fault offsets vertically the bedrock, alluvial fan, river terraces and travertine platform. On the upthrown side of the fault, there are 4 prominent fault facets, which are ～600m, ～400m, ～200m, and ～80m above the surface of piedmont plain, respectively. At the base of fault facets, sustained faulting has given rise to the formation of east facing fault scarps and surface ruptures that cut the terraces, alluvial fans and travertine platform. Leveling survey and in situ measurement with tape measure show that the 6 sets of fault scarps are about 0 3～0.6m, 4～5m, 8±1m, 15±3m, 24±4m and 45±5m in height, respectively, and that the higher the scarp, the older the strata cut by the scarp. Among them, the 0.3～0.6m high fault scarp might be associated with M S 6～7 earthquake of middle late Holocene, the 4～5m and 8±1m fault scarps offset separately the terraces Ⅰ and Ⅱ, while the 15±3m, 24±4m and 45±5m high fault scarps offset separately the terrace Ⅲ, Ⅳ, Ⅴ and travertine platform. U series dating results indicate that the fault scarp that offsets the terracesⅠand Ⅱ was formed 11～7ka BP, the scarp that offsets the terraces Ⅲ was formed 21～25ka BP, and the scarps that offset the terrace Ⅳ and Ⅴ and the correlated travertine platform were formed 45 2～53 6ka BP and 103～127ka BP, respectively. The 80～200m high scarps might be formed since 324～521ka BP. Moreover, the dating results suggest also that the average vertical slip rate along the normal fault on the western side of the Wenquan graben is 0.45mm/a with the maximum value of less than 1.2mm/a. The relief across the normal fault indicates that the minimum cumulative displacement on the fault is about 2.1km. The maximum cumulative throws on the fault is about 8.2km. The trenching across the fault revealed that at least 3 paleoseismic events have occurred along the fault since late Pleistocene. The magnitude of those events can be estimated to be M S 6～7 and the approximate recurrence interval to be from about 400 to 3000yr. The slip rate on normal fault from Wenquan graben implies that the east west extension rate absorbed by a single graben in central Tibet is significantly lower than that of the grabens in southern Tibet, but this does not imply that the east west extension rate in central Tibet must be significantly lower than that in southern Tibet. This is because that the east west extension in central Tibet might be accommodated by a larger number of normal and strike slip faults distributed in this area. On the basis of the total cumulative throws and the average vertical slip rate on the fault, it is inferred that the initiation time of the normal faulting to be at about 18 2～1 8Ma BP. The broad similarities in the magnitude of slip, the direction of extension and the initiation time of normal faulting in both central and southern Qinghai Tibet Pateau imply that the east west extension within the Qinghai Tibet Plateau has occurred synchronously, and that the crustal thickness in central and southern Tibet Plateau has reached its maximum value since Miocene, while the whole Plateau has reached its present elevation.
引文
[1]《唐古拉山幅1/20万区域地质图》,1990—1993年,由青海省区域综合地质大队六分队实测。
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吴中海,赵希涛,江万,等.2003.念青唐古拉山东南麓更新世冰川沉积物年龄测定的初步结果[J].冰川冻土,25(3):272—274.
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崔之久,高全洲,刘耕年,等.1996.夷平面、古岩溶与青藏高原隆升[J].中国科学(D辑),26(4):378—385.
CUIZhi jiu,GAOQuan zhou,LIUGeng nian,etal.1996.Planationsurface,palaeokarstandupliftofXizang(Tibet)Plateau[J].ScienceinChina(SerD),39(4):391—440.
邓起东,汪一鹏,廖玉华.1984.断层崖崩积楔及贺兰山山前断裂全新世活动历史[J].科学通报,(9):557—560.
DENGQi dong,WANGYi peng,LIAOYu hua.1984.ColluvialwedgeoffaultscarpsandHolocenefaultingonHelanshanrange frontfault[J].ChineseScienceBulletin,(9):557—560(inChinese).
邓起东,于贵华,叶文华.1992.地震地表破裂参数与震级关系的研究[A].见:国家地震局地质研究所编.活动断裂研究(2).北京:地震出版社.247—264.
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樊溶河,吴锡浩.1982.青南藏北高原第四纪冰期堆积物的水文地质特征概述[A].见:地质矿产部青藏高原地质文集编委会编.青藏高原地质文集(4).北京:地质出版社.87—99.
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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[J].中国科学(B辑),9(6):608—616.
LIJi jun,WENShi xuan,ZHANGQing song,etal.1979.Adiscussionontheperiod,amplitudeandtypeoftheupliftoftheQinghaiXizangPlateau[J].ScienceinChina(SerB),9(6):608—616(inChinese).
李吉均,方小敏,马海洲,等.1996.晚新生代黄河上游演化与青藏高原隆起[J].中国科学(D辑),26:316—322.
LIJi jun,FANGXiao min,MAHai zhou,etal.1996.GeomorphologicalandenvironmentalevolutionoftheYellowRiverduringthelateCenozoic[J].ScienceinChina(SerD),39(4):380—390.
施雅风.1998.第四纪中期青藏高原冰冻圈的演化及其与全球变化的联系[J].冰川冻土,20(3):197—207.
SHIYa feng.1998.EvolutionofthecryosphereintheTibetanPlateau,China,anditsrelationshipwiththeglobalchangeintheMidQuaternary[J].JournalofGlaciologyandGeocryology,20(3):197—207(inChinese).
吴章明,汪一鹏,任金卫,等.1993.青藏高原北部金沙江、澜沧江缝合带晚第四纪的活动性[J].地震地质,15(1):28—31.
WUZhang ming,WANGYi peng,RENJin wei,etal.1993.ActivityoftheJinshaandLancangsuture,northernQinghaiXizangPlateauinlateQuaternary[J].SeismologyandGeology,15(1):28—31(inChinese).
吴中海,赵希涛,江万,等.2003.念青唐古拉山东南麓更新世冰川沉积物年龄测定的初步结果[J].冰川冻土,25(3):272—274.
WUZhong hai,ZHAOXi tao,JIANGWan,etal.2003.DatingresultofthePleistoceneglacialdepositsonthesoutheastfootofNyaiqentanglhaMountains[J].JournalofGlaciologyandGeocryology,25(3):272—274(inChinese).
钟大赉,丁林.1996.青藏高原的隆起过程及其机制探讨[J].中国科学(D辑),26(4):289—295.
ZHONGDa lai,DINGLin.1996.RisingprocesssoftheQinghaiXizang(Tibet)Plateauanditsmechanism[J].ScienceinChina(SerD),39(4):369—379.
AnZhisheng,JohnEK ,WarrenLP ,etal.2001.EvolutionofAsianmonsoonsandphasedupliftoftheHimalayanTibetanPlateausinceLateMiocenetimes[J].Nature,411:62—66.
ArmijoR ,TapponnierP ,MercierJL ,etal.1986.QuaternaryextensioninsouthTibet:Fieldobservationsandtectonicim plications[J].JourGeophysRes,91(B14):13803—13872.
ArmijoR ,TapponnierP ,HanT .1989.LateCenezoicright lateralstrike slipfaultinginsouthernTibet[J].JourGeophysRes,94:2787—2838.
BlisniukPM ,BradleyRH ,JohannesG ,etal.2001.NormalfaultingincentralTibetsinceatleast13.5Myrago[J].Na ture,412:628—632.
BlisniukPM ,SharpWD .2003.RatesoflateQuaternarynormalfaultingincentralTibetfromU seriesdatingofpedogeniccarbonateindisplacedfluvialgraveldeposits[J].EarthPlanetSciLett,215:169—186.
CoganM ,NelsonKD ,KiddWSF ,etal.1998.ShallowstructureoftheYadongGulurift,southernTibet,fromrefractionanalysisofProjectINDEPTHcommonmidpointdata[J].Tectonics,17(1):46—61.
ColemanM ,HodgesK .1995.EvidenceforTibetanPlateauupliftbefore14Myragofromanewminimumestimateforeast westextension[J].Nature,374:49—52.
DeweyJF ,ShackletonRM ,ChangChengfa,etal.1988.ThetectonicevolutionoftheTibetanPlateau[J].PhilTransRSocLond(SerA),327:379—413.
HarrisonTM ,CopelandP ,KiddWSF ,etal.1992.RaisingTibet[J].Science,225:1663—1670.
KiddWSF ,MolnarP .1988.Quaternaryandactivefaultingobservedonthe1985AcademiaSinicaRoyalSocietygeotra verseofTibet[J].PhilTransRSocLondon(SerA),327:337—363.
LiJijun.1995.UpliftofQinghaiXizang(Tibet)PlateauandGlobalChange[M].LanzouUniversityPress,Lanzhou.MolnarP ,TapponnierP .1975.CenozoictectonicsofAsia:effectsofacontinentalcollision[J].Science,189:418—426.
MolnarP ,TapponnierP .1978.ActivetectonicsofTibet[J].JourGeophysRes,83:5361—5375.
MolnarP ,EnglandP .1990.LateCenozoicupliftofmountainrangesandglobalclimatechange:Chickenoregg[J].Na ture,346:29—34.
NelsonKD ,ZhaoW ,BrownLD ,etal.1996.PartiallymoltenmiddlecrustbeneathsouthernTibet:SynthesisofProjectINDEPTHresults[J].Science,174:1684—1688.
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