从水系的分布形态探讨沂沭断裂带的运动特征
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摘要
郯城—庐江断裂带是纵贯中国大陆东部,长达2 000km以上的大断裂带。该研究利用DEM数据和ETM,以及谷歌卫星影像来分析郯城—庐江断裂带中段的沂沭断裂带周边的水系的几何分布形态特征。三维卫星图像解译和野外调查的结果显示:(1)沿断裂带周边发育的水系的几何分布形态主要受由F1—F44条主要断层所组成的沂沭断裂带构造所制约;(2)沿断裂带发育的水系不具有典型的走滑断层的系统化的同步转折和位错的变形特征;(3)沂沭断裂带东侧的F1和F2断裂是现今的活动断裂,而F3和F4断裂在第四纪基本没有明显的活动迹象;(4)F1和F2断裂以垂向运动为主,具有高角度的逆断层或正断层的运动特征。该研究结果显示沿断裂发育的水系地貌和几何分布特征可作为评价断裂的活动性和运动特征的地貌标志。
The Yishu Fault Zone,the central segment of the Tan Lu Fault Zone(TLFZ),located in Shandong Peninsula,eastern China,is composed of four major faults,called F1 F4 from east to west,forming a 50-km-wide zone.In this study,we analyzed the distribution pattern of drainage systems developed along the Yishu Fault Zone mainly on the basis of the interpretations of Digital Elevation Model(DEM) data,Landsat Enhanced Thematic Mapper(ETM),and Google imagery data and field investigations.Our results reveal that the streams and gullies are mainly restricted by the Yishu Fault Zone along the graben structures bounded by F1 F2 and F3 F4 faults,respectively,in the northern segment of the Yishu Fault Zone,and are constrained by F1 and F2 faults but not by F3 and F4 faults in the southern segment.Geologic and topographic evidence shows that the Yishu Fault Zone is characterized by the deformational features of normal-reverse faults with high dip angle of 70°-90° and that F1 and F2 faults are currently active but F3 and F4 faults are inactive in the Quaternary.Our results confirm that the topographic features of drainage systems are reliable indicators of ground deformation along the pre-existing fault structures and can be used for studying the activity and dynamic characteristics of active faults.
The Yishu Fault Zone,the central segment of the Tan Lu Fault Zone(TLFZ),located in Shandong Peninsula,eastern China,is composed of four major faults,called F1 F4 from east to west,forming a 50-km-wide zone.In this study,we analyzed the distribution pattern of drainage systems developed along the Yishu Fault Zone mainly on the basis of the interpretations of Digital Elevation Model(DEM) data,Landsat Enhanced Thematic Mapper(ETM),and Google imagery data and field investigations.Our results reveal that the streams and gullies are mainly restricted by the Yishu Fault Zone along the graben structures bounded by F1 F2 and F3 F4 faults,respectively,in the northern segment of the Yishu Fault Zone,and are constrained by F1 and F2 faults but not by F3 and F4 faults in the southern segment.Geologic and topographic evidence shows that the Yishu Fault Zone is characterized by the deformational features of normal-reverse faults with high dip angle of 70°-90° and that F1 and F2 faults are currently active but F3 and F4 faults are inactive in the Quaternary.Our results confirm that the topographic features of drainage systems are reliable indicators of ground deformation along the pre-existing fault structures and can be used for studying the activity and dynamic characteristics of active faults.
引文
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[26]Xu J W,Zhu G.Tectonic models of the Tan-Lu Fault Zone,Eastern China[J].International Geological Review,1994,36:771-784.
[27]Wan T F,Zhu H,Zhao L,et al.Formation and evolution of the Tancheng-Lujiang fault zone:A synthesis[M]∥Zhao Y H.Formation and Evolution of the Tancheng-Lujiang Fault Zone.Wuhan:China University of Geosciences Press,1996:1-11.
[28]Wan T F.Tectonics of China:Data,Maps and Evolution[M].Beijing:Higher Education Press;Dordrecht Heidel-berg:Springer,2011:1-501.
[29]Xu J.The Tancheng-Lujiang Wrench Fault System[M].England:Willy&Sons,1993:279.
[30]国家地震局地质研究所.郯庐断裂[M].北京:地震出版社,1987:254.
[31]Mercier J L,Hou M J,Vergély P,et al.Structural and stra-tigraphical constraints on the kinematics history of the South-ern Tan-Lu Fault Zone during the Mesozoic,Anhui Province,China[J].Tectonophysics,2007,439:33-66.
[32]Lin A,Miyata T,Wan T.Tectonic characteristics of the central segment of the Tancheng-Lujiang fault zone in the central segment,Shandong Peninsula,eastern China[J].Tectonophysics,1998,293:85-104.
[33]曾秋生.郯庐断裂带新生代的活动及应力场特征[M]∥中国活动断裂.北京:地震出版社,1982:101-105.
[34]江娃利,刘仲温,李成业,等.山东沂沭断裂带全新世断层展布及运动特征[M]∥中国活动断层研究.北京:地震出版社,1994:146-153.
[35]Huang W.Morphologic patterns of stream channels on the active Yishu Fault,southern Shandong Province,Eastern China:Implications for repeated great earthquakes in the Holocene[J].Tectonophysics,1993,219:218-304.
[36]Lin A,Fu B,Guo J,et al.Co-seismic strike-slip and rupture length produced by the2001MS8.1Central Kunlun earth-quake[J].Science,2002,296:2015-2017.
[2]Lin A,Yang Z,Sun Z,et al.Tectonic relationship betweenthe course change of the Yangtze River and Indo-Asia colli-sion[M]∥Landowe S J,Hammler G M.Structural Geology:New Research.Hauppauge NY:Nova Science PublishersInc.2008.
[3]Wallace R E.Notes on Stream Channels Offset by the SanAndreas Fault,Southern Coast Ranges,California[C].Dick-inson:School of Earth Sciences,Stanford University,1968.
[4]Wallace R E.The San Andreas Fault System,California[R].Professional Paper,Vol 1515.Washington DC:US Geolog-ical Survey,1990.
[5]Jackson J,Norris R,Yongson J.The structural evolution ofactive faults and fold systems in central Otago,New Zealand:Evidence revealed by drainage patterns[J].Journal Structureof Geology,1996,18:217-234.
[6]Lacassin R,Replumaz A,Leloup P H.Hairpin river loopsand slip-sense inversion on southeast Asian strike-slip faults[J].Geology,1998,26:703-706.
[7]Maruyama T,Lin A.Tectonic history of the Rokko activefault zone(southwest Japan)as inferred from cumulative off-sets of stream channels and basement rocks[J].Tectono-physics,2000,323:197-216.
[8]Maruyama T,Lin A.Active strike-slip faulting history in-ferred from topographic features and basement rocks:A casestudy of the Arima-Takatsuki Tectonic Line,southwest Ja-pan[J].Tectonophysics,2002,344:81-101.
[9]Maruyama T,Lin A.Slip sense inversion on active strike-slipfaults in southwest Japan and its implications for Cenozoictectonic evolution[J].Tectonophysics,2004,383:45-70.
[10]Lin A,Fu B,Kano K,et al.Late Quaternary right-lateraldisplacement along active faults in the Yanqi Basin,southernTianshan,northwest China[J].Tectonophysics,2002,354:157-178.
[11]Matsuda T.Strike-slip faulting along the Atotsugawa fault,Japan[J].Bulletin of Earthquake Research Institute,theUniversity of Tokyo,1966,44:1179-1212(in Japanese withEnglish abstract).
[12]Leloup P H,Lacassin R,Tapponnier P,et al.The AilaoShan Red River shear zone(Yunnan China),Tertiary trans-form boundary of Indochina[J].Tectonophysics,1995,251:3-84.
[13]Lin A,Guo J,Kano K,et al.Average slip rate and recur-rence interval of large-magnitude earthquakes on the westernsegment of the strike-slip Kunlun fault,northern Tibet[J].Bulletin of Seismological Society of America,2006,96:1597-1611.
[14]Cowie P A,Scolz C H.Growth of faults by accumulation ofseismic slip[J].Journal of Geophysical Research,1992,97:11085-11095.
[15]Schumm S,Dumont J F,Holbrook J M.Active Tectonicsand Alluvial Rivers[M].London:Cambridge UniversityPress,2000:276.
[16]Sieh K E,Jahns R H.Holocene activity of the San AndreasFault at Wallace Creek,California[J].Geological Society ofAmerican Bulletin,1984,95:883-896.
[17]Gaudemer Y,Tapponnier P,Turcotte D L.River offsetsacross active strike-slip faults[J].Annales Tectonica,1989,3:55-76.
[18]Bellier O,Sёrbrier M.Is the slip rate variation on the GreatSumatoran Fault accommodated by fore-arc stretching[J]?Geophysical Research Letters,1995,22:1969-1972.
[19]Delcaillau B,Defofontanines B,Floissac L,et al.Morpho-tectonic evidence from lateral propagation of active frontalfold,Pakuashan anticline,foothills of Taiwan[J].Geomor-phology,1998,24:263-290.
[20]Gupta S.Himalayan drainage patterns and the origin of fluvi-al megafans in the Ganges foreland basin[J].Geology,1997,25:11-14.
[21]Keller E A,Printer N.Active Tectonics:Earthquakes,Up-lift,and Landscape[M].2nd ed.New Jersey:Prentice Hall,2002.
[22]Paton S.Active normal faulting,drainage patterns,and sedi-mentation in southwestern Turkey[J].Journal of GeologicalSociety of London,1992,149:1031-1044.
[23]Leeder M R,Gawthorpe R L.Sedimentary models for exten-sional tilt-block/half-graben basins[M]∥Coward M P.Con-tinental Extensional Tectonics.Geological Society SpecialPublication,1987,28:139-152.
[24]Alexander L,Leeder M R.Geomorphlogy and surface tiltingin an active extensional basin,SW Montana,USA[J].Jour-nal of Geological Society of London,1990,147:461-467.
[25]徐嘉炜.郯城—庐江深断裂带的平移运动[J].华东地质,1964(5):17-34.
[26]Xu J W,Zhu G.Tectonic models of the Tan-Lu Fault Zone,Eastern China[J].International Geological Review,1994,36:771-784.
[27]Wan T F,Zhu H,Zhao L,et al.Formation and evolution of the Tancheng-Lujiang fault zone:A synthesis[M]∥Zhao Y H.Formation and Evolution of the Tancheng-Lujiang Fault Zone.Wuhan:China University of Geosciences Press,1996:1-11.
[28]Wan T F.Tectonics of China:Data,Maps and Evolution[M].Beijing:Higher Education Press;Dordrecht Heidel-berg:Springer,2011:1-501.
[29]Xu J.The Tancheng-Lujiang Wrench Fault System[M].England:Willy&Sons,1993:279.
[30]国家地震局地质研究所.郯庐断裂[M].北京:地震出版社,1987:254.
[31]Mercier J L,Hou M J,Vergély P,et al.Structural and stra-tigraphical constraints on the kinematics history of the South-ern Tan-Lu Fault Zone during the Mesozoic,Anhui Province,China[J].Tectonophysics,2007,439:33-66.
[32]Lin A,Miyata T,Wan T.Tectonic characteristics of the central segment of the Tancheng-Lujiang fault zone in the central segment,Shandong Peninsula,eastern China[J].Tectonophysics,1998,293:85-104.
[33]曾秋生.郯庐断裂带新生代的活动及应力场特征[M]∥中国活动断裂.北京:地震出版社,1982:101-105.
[34]江娃利,刘仲温,李成业,等.山东沂沭断裂带全新世断层展布及运动特征[M]∥中国活动断层研究.北京:地震出版社,1994:146-153.
[35]Huang W.Morphologic patterns of stream channels on the active Yishu Fault,southern Shandong Province,Eastern China:Implications for repeated great earthquakes in the Holocene[J].Tectonophysics,1993,219:218-304.
[36]Lin A,Fu B,Guo J,et al.Co-seismic strike-slip and rupture length produced by the2001MS8.1Central Kunlun earth-quake[J].Science,2002,296:2015-2017.
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