南沙海槽前陆盆地热结构
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摘要
岩石圈热结构直接影响着岩石的物理性质和流变学性质,从而制约着岩石圈的形成演化。在研究南沙海槽前陆盆地地质构造背景和岩石圈热结构影响参数基础上,文章采用一维稳态热传导方程模拟计算并获得了盆地94N05地震剖面岩石圈热结构。计算表明,盆地区域大地热流平均值约为62mW.m 2;地幔热流值约37—44mW.m 2,对地表热流贡献达60%—70%。南沙海槽前陆盆地处于构造热恢复阶段,地表热流受中中新世挤压构造环境影响相对较低且主要受深部地幔控制,莫霍面温度介于500—600℃,热岩石圈较薄,厚度约60—70km。通过计算岩石圈热结构及居里面深度特征揭示揭示盆地深部岩石圈温度较高以及热活动稳定可能是南沙群岛海域地震发生很少的重要原因。
Thermal structure of continental lithosphere can directly affect physical and rheological properties of rock,thus limiting the evolution of lithosphere.Based on tectonic setting and influencing parameters of lithospheric thermal state in the Nansha Trough Foreland,we numerically simulated lithospheric thermal structure of 94N05 seismic profile in the basin using an one-dimensional steady-state heat-conduction equation.Simulation Results show that average heat flow is about 62 mW·m 2 in the basin,and mantle heat flow is between 37 and 44 mW·m 2,which is up to 60% 70% of the surface heat flow. The Nansha Trough Foreland Basin is in the tectonic thermal recovering phase.Affected by compressional tectonic surroundings since the Miocene,the surface heat flow is relatively low and mainly controlled by deep mantle,and temperature of Moho varies from 500 to 600℃.Thickness of thermal lithosphere is as thin as 60 70 km.This research also reveals that key factors of few regional earthquakes may be related to high temperature and thermal stabilization of the deep lithosphere in the Nansha Islands waters.
Thermal structure of continental lithosphere can directly affect physical and rheological properties of rock,thus limiting the evolution of lithosphere.Based on tectonic setting and influencing parameters of lithospheric thermal state in the Nansha Trough Foreland,we numerically simulated lithospheric thermal structure of 94N05 seismic profile in the basin using an one-dimensional steady-state heat-conduction equation.Simulation Results show that average heat flow is about 62 mW·m 2 in the basin,and mantle heat flow is between 37 and 44 mW·m 2,which is up to 60% 70% of the surface heat flow. The Nansha Trough Foreland Basin is in the tectonic thermal recovering phase.Affected by compressional tectonic surroundings since the Miocene,the surface heat flow is relatively low and mainly controlled by deep mantle,and temperature of Moho varies from 500 to 600℃.Thickness of thermal lithosphere is as thin as 60 70 km.This research also reveals that key factors of few regional earthquakes may be related to high temperature and thermal stabilization of the deep lithosphere in the Nansha Islands waters.
引文
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[21]施小斌,周蒂,张毅祥.南海北部陆缘岩石圈热-流变结构[J].科学通报,2000,45(15):1660-1665.
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[24]CERMAK V.Crustal heat production and mantle heat flowin Central and Eastern Europe[J].Tectonophysics,1989,159(3/4):195-215.
[25]SHI X,ZHOU D,QIU X,et al.Thermal and rheologicalstructures of the Xisha Trough,South China Sea[J].Tectonophysics,2002,351(4):285-300.
[26]CERMAK V,BODRI L.A heat production model of thecrust and upper mantle[J].Tectonophysics,1991,194(4):307-323.
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[29]POLLACK H,CHAPMAN D.On the regional variation ofheat flow,geotherms,and lithospheric thickness[J].Tectonophysics,1977,38(3/4):279-296.
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[31]GARCIA-CASTELLANOS D,FERNANDEZ M,TORNEM.Modeling the evolution of the Guadalquivir forelandbasin(southern Spain)[J].Tectonics,2002,21(3):1-17.
[32]ZIELINSKI G,BJOROY M,ZIELINSKI R,et al.Heat flowand surface hydrocarbons on the Brunei continentalmargin[J].AAPG bulletin,2007,91(7):1053-1080.
[33]RAI S,THIAGARAJAN S.2-D Crustal thermal structurealong Thuadara-Sindad DSS profile across Narmada-Sonlineament,central India[J].Journal of Earth System Science,2007,116(4):347-355.
[34]吴招才,高金耀,赵俐红,等.南海北部陆缘的磁异常特征及居里面深度[J].地球科学:中国地质大学学报,2010,(06):1060-1068.
[35]胡旭芝,徐鸣洁,谢晓安,等.中国东北地区航磁特征及居里面分析[J].地球物理学报,2006,(6):1674-1681.
[36]赵俊峰,施小斌,丘学林,等.南海东北部居里面特征及其石油地质意义[J].热带海洋学报,2010,29(1):126-131.
[2]GOES S,SIMONS F J,YOSHIZAWA K.Seismicconstraints on temperature of the Australian uppermostmantle[J].Earth and Planetary Science Letters,2005,236(1/2):227-237.
[3]NORDEN B,F RSTER A,BALLING N.Heat flow andlithospheric thermal regime in the Northeast GermanBasin[J].Tectonophysics,2008,460(1/4):215-229.
[4]吴耀,金振民,欧新功,等.中国大陆科学钻探(CCSD)主孔地区岩石圈热结构[J].岩石学报,2005,(02):439-450.
[5]安美建,石耀霖.中国大陆地壳和上地幔三维温度场[J].中国科学:D辑地球科学,2007,37(06):736-745.
[6]张健,汪集旸.南海北部大陆边缘深部地热特征[J].科学通报,2000,45(10):1095-1100.
[7]ZHOU D,YAO B.Tectonics and sedimentary basins of theSouth China Sea:Challenges and progresses[J].Journal ofEarth Science,2009,20(1):1-12.
[8]YAN P,LIU H.Tectonic-stratigraphic division and blind foldstructures in Nansha Waters,South China Sea[J].Journal ofAsian Earth Sciences,2004,24(3):337-348.
[9]TAYLOR B,HAYES D.Origin and history of the SouthChina Sea basin[M].Washington,D C:AmericanGeophysical Union,1983,23-56.
[10]INGRAM G,CHISHOLM T,GRANT C,et al.DeepwaterNorth West Borneo:hydrocarbon accumulation in an activefold and thrust belt[J].Marine and Petroleum Geology,2004,21(7):879-887.
[11]HESSE S,BACK S,FRANKE D.The deep-waterfold-and-thrust belt offshore NW Borneo:Gravity-drivenversus basement-driven shortening[J].Geological Society ofAmerica Bulletin,2009,121(5-6):939-953.
[12]吴世敏,周蒂,刘海龄.南沙地块构造格局及其演化特征[J].大地构造与成矿学,2004,28(1):23-28.
[13]苏达权,黄慈流,夏戡原.论南沙海槽的地壳性质[J].地质科学,1996,31(04):409-415.
[14]FRANKE D,BARCKHAUSEN U,HEYDE I,et al.Seismicimages of a collision zone offshore NW Sabah/Borneo[J].Marine and Petroleum Geology,2008,25(7):606-624.
[15]金庆焕,李唐根.南沙海域区域地质构造[J].海洋地质与第四纪地质,2000,20(1):1-8.
[16]刘绍文,王良书,龚育龄,等.济阳坳陷岩石圈热-流变学结构及其地球动力学意义[J].中国科学:D辑地球科学,2005,35(03):203-214.
[17]SHI X,QIU X,XIA K,et al.Characteristics of surface heatflow in the South China Sea[J].Journal of Asian EarthSciences,2003,22(3):265-277.
[18]BRIAIS A,PATRIAT P,TAPPONNIER P.Updatedinterpretation of magnetic anomalies and seafloor spreadingstages in the South China Sea:implications for the Tertiarytectonics of Southeast Asia[J].Journal of GeophysicalResearch,1993,98(B4):6299-6328.
[19]刘绍文,王良书,李成,等.塔里木北缘岩石圈热-流变结构及其地球动力学意义[J].中国科学:D辑地球科学,2003,33(09):852-863.
[20]赵平,汪集旸,汪缉安,等.中国东南地区岩石生热率分布特征[J].岩石学报,1995,11(03):292-305.
[21]施小斌,周蒂,张毅祥.南海北部陆缘岩石圈热-流变结构[J].科学通报,2000,45(15):1660-1665.
[22]BIRCH F.Heat from radioactivity[M].New York:JohnWiely&Sons,1954:148-174.
[23]LACHENBRUCH A.Crustal temperature and heatproduction:implications of the linear heat-flow relation[J].Journal of Geophysical Research,1970,75(17):3291-3300.
[24]CERMAK V.Crustal heat production and mantle heat flowin Central and Eastern Europe[J].Tectonophysics,1989,159(3/4):195-215.
[25]SHI X,ZHOU D,QIU X,et al.Thermal and rheologicalstructures of the Xisha Trough,South China Sea[J].Tectonophysics,2002,351(4):285-300.
[26]CERMAK V,BODRI L.A heat production model of thecrust and upper mantle[J].Tectonophysics,1991,194(4):307-323.
[27]BUNTEBARTH G.Geothermics:an introduction[M].NewYork:Springer-Verlag,1984,1-144.
[28]欧新功,金振民,夏斌,等.利用超高压变质岩的P波速度估算地下岩石的热导率[J].地球科学,2006,31(04):564-568.
[29]POLLACK H,CHAPMAN D.On the regional variation ofheat flow,geotherms,and lithospheric thickness[J].Tectonophysics,1977,38(3/4):279-296.
[30]臧绍先,刘永刚,宁杰远.华北地区岩石圈热结构的研究[J].地球物理学报,2002,45(01):56-66.
[31]GARCIA-CASTELLANOS D,FERNANDEZ M,TORNEM.Modeling the evolution of the Guadalquivir forelandbasin(southern Spain)[J].Tectonics,2002,21(3):1-17.
[32]ZIELINSKI G,BJOROY M,ZIELINSKI R,et al.Heat flowand surface hydrocarbons on the Brunei continentalmargin[J].AAPG bulletin,2007,91(7):1053-1080.
[33]RAI S,THIAGARAJAN S.2-D Crustal thermal structurealong Thuadara-Sindad DSS profile across Narmada-Sonlineament,central India[J].Journal of Earth System Science,2007,116(4):347-355.
[34]吴招才,高金耀,赵俐红,等.南海北部陆缘的磁异常特征及居里面深度[J].地球科学:中国地质大学学报,2010,(06):1060-1068.
[35]胡旭芝,徐鸣洁,谢晓安,等.中国东北地区航磁特征及居里面分析[J].地球物理学报,2006,(6):1674-1681.
[36]赵俊峰,施小斌,丘学林,等.南海东北部居里面特征及其石油地质意义[J].热带海洋学报,2010,29(1):126-131.
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