东海陆坡及邻近槽底天然气水合物成藏条件分析及前景
摘要
在西太平洋边缘海中,东海是唯一没有获得天然气水合物样品的边缘海。利用已有的地震资料、海底温度资料等,从沉积物来源、沉积地层厚度、烃源岩条件、沉积速率、海底温度—压力条件等方面对东海水合物成藏条件进行了分析。认为冲绳海槽沉积物源丰富,沉积厚度大,且发育烃源岩地层。冲绳海槽较高的沉积速率主要分布于冲绳海槽槽底沉积中心,以及西部陆坡连接海底峡谷底部的三角洲区域。根据冲绳海槽实测的海底温度数据,整个冲绳海槽地区600m以深的范围都能够满足水合物发育的温度、压力条件。以温度梯度为30℃/km计算,冲绳海槽中水合物稳定域的最大厚度为650m。冲绳海槽盆地中普遍发育的底辟构造、背斜构造等局部构造,以及网格状断裂系统,为烃类气流体的向上及侧向运移创造了有利条件,成为天然气水合物发育的有利区带。根据已经发现的BSR特征来看,东海地区天然气水合物前景广阔。
Up to now,East China Sea is the only marginal sea in which gas hydrate samples haven't been revealed in the West Pacific.Based on the geological and geophysical data obtained both from our past several cruises and from other publications,geological factors including sedimentary sources,sedimentary thickness,source rock,sedimentation rate,temperature and pressure distribution that control gas hydrate development have been analysed.The paper points out that East China Sea has abundant sedimentary sources supplied mainly by Changjiang River and partly by Huanghe River which have the capability of transporting 1,498×106 t of sediment each year from mainland China to East China Sea,Bohai Sea and Huanghai Sea.Several sedimentary centers have been clearly revealed along East China Sea Slope and west part of Okinawa Trough by our seismic data.Sediment thicknesses of those centers are all over 5 km with the earliest sediment layer since around Eocene or even Oligocene time.We believe that source rock is existing among the deeper part of the sediment center either Eocene layer or Oligocene layer which have already been confirmed as good quality source rock in East China Shelf Basin by drilling works,and hydrocarbons might be generated earlier from the source rock in those centers than in shelf basin due to higher temperature gradient in slope and trough area as comparing with that of the shelf area.Sedimentation rate along the slope and trough varies from several cm/ka to 400 cm/ka,with higher values mainly constraining in the sediment centers and delta area which is connecting to the end of slope canyons and distributing at the most west part of trough basin.Based on our measured sea floor temperature data,gas hydrates can only developed in the slope and trough area with water depth over than 600 m.Gas hydrates stability zone can be as thick as 650 m when take temperature gradient as 30 ℃/km,but thinning to northeast along the axis of Okinawa Trough and to northwest up to the slope as the water depth changing shallower and sea floor temperature changing warmer.Local geological structures like mud diapir,anticline,fracture system are quite common in the study area,and they mainly control the fluid migration forming a favorable environment for the gas hydrate development and preservation in the study area.Based on our analysis,and BSRs found on some seismic profiles,we believe that the reason for gas hydrates unrevealling in East China Sea as comparing with other marginal seas is mainly due to the relatively lower exploration level.
Up to now,East China Sea is the only marginal sea in which gas hydrate samples haven't been revealed in the West Pacific.Based on the geological and geophysical data obtained both from our past several cruises and from other publications,geological factors including sedimentary sources,sedimentary thickness,source rock,sedimentation rate,temperature and pressure distribution that control gas hydrate development have been analysed.The paper points out that East China Sea has abundant sedimentary sources supplied mainly by Changjiang River and partly by Huanghe River which have the capability of transporting 1,498×106 t of sediment each year from mainland China to East China Sea,Bohai Sea and Huanghai Sea.Several sedimentary centers have been clearly revealed along East China Sea Slope and west part of Okinawa Trough by our seismic data.Sediment thicknesses of those centers are all over 5 km with the earliest sediment layer since around Eocene or even Oligocene time.We believe that source rock is existing among the deeper part of the sediment center either Eocene layer or Oligocene layer which have already been confirmed as good quality source rock in East China Shelf Basin by drilling works,and hydrocarbons might be generated earlier from the source rock in those centers than in shelf basin due to higher temperature gradient in slope and trough area as comparing with that of the shelf area.Sedimentation rate along the slope and trough varies from several cm/ka to 400 cm/ka,with higher values mainly constraining in the sediment centers and delta area which is connecting to the end of slope canyons and distributing at the most west part of trough basin.Based on our measured sea floor temperature data,gas hydrates can only developed in the slope and trough area with water depth over than 600 m.Gas hydrates stability zone can be as thick as 650 m when take temperature gradient as 30 ℃/km,but thinning to northeast along the axis of Okinawa Trough and to northwest up to the slope as the water depth changing shallower and sea floor temperature changing warmer.Local geological structures like mud diapir,anticline,fracture system are quite common in the study area,and they mainly control the fluid migration forming a favorable environment for the gas hydrate development and preservation in the study area.Based on our analysis,and BSRs found on some seismic profiles,we believe that the reason for gas hydrates unrevealling in East China Sea as comparing with other marginal seas is mainly due to the relatively lower exploration level.
引文
[1]Shoji H,Soloviev V,Matveeva T.Hydrate-bearing structures inthe sea of Okhotsk[J].EOS,2005,86:13-24.
[2]栾锡武,赵克斌,Obzhirov A,等.鄂霍次克海浅表层天然气水合物的勘查识别和基本特征[J].中国科学(D辑),2008,38(1):99-107.
[3]秦蕴珊,赵一阳,陈丽蓉.东海地质[M].北京:科学出版社,1987.
[4]金翔龙.东海海洋地质[M].北京:海洋出版社,1992.
[5]许东禹.中国东海地质[M].北京:地震出版社,1997.
[6]贾健谊,顾惠荣.东海西湖凹陷含油气系统与油气资源评价[M].北京:地质出版社,2002:204.
[7]李巍然,杨作升,王琦,等.冲绳海槽陆源碎屑峡谷通道搬运与海底扇沉积[J].海洋与湖沼,2001,32(4):371-380.
[8]栾锡武,高金耀,梁瑞才,等.冲绳海槽宫古段中央地堑的形态与分布[J].地质学报,2006,80(8):1149-1155.
[9]栾锡武,岳保静.冲绳海槽宫古段中央地堑中的火山分布及地质意义[J].海洋与湖沼,2007,38(3):266-271.
[10]栾锡武,秦蕴珊,张训华,等.东海陆坡及相邻槽底天然气水合物的稳定域分析[J].地球物理学报,2003,46(4):467-475.
[11]赵一阳,何丽娟,张秀莲.冲绳海槽沉积物地球化学的基本特征[J].海洋与湖沼,1984,15(4):371-379.
[12]吴明清,王贤觉.东海沉积物的稀土和微量元素[J].地球化学,1991,20(1):40-46.
[13]杜德文,孟宪伟,王永吉.沉积物物源组成的定量判识方法及其在冲绳海槽的应用[J].海洋与湖沼,1999,30(6):532-539.
[14]苟淑名.冲绳海槽表层沉积物孢粉组合特征[J].海洋科学,1982,6:14-18.
[15]李凡,张秀荣,李永植.南黄海埋藏古三角洲[J].地理学报,1998,53(3):238-244.
[16]谢钦春,叶银灿,陆炳火.东海陆架坡折地形和沉积作用过程[J].海洋学报,1984,6(1):61-71.
[17]茅志昌,李九发,吴华林.上海市滩涂促淤圈围研究[J].泥沙研究,2003,(2):77-81.
[18]任美锷.黄河的输沙量:过去、现在和将来——距今15万年以来的黄河泥沙收支表[J].地球科学进展,2006,21(6):551-563.
[19]戴仕宝,杨世伦,蔡爱民.51年来珠江流域输沙量的变化[J].地理学报,2007,62(5):545-554.
[20]蒋富清,李安春,李铁刚.冲绳海槽北端表层沉积物过渡元素地球化学特征[J].海洋与湖沼,2006,37(1):75-83.
[21]赵金海,唐建,薄玉玲.关于东海新生代盆地油气勘探的若干见解[J].中国海上油气(地质),2003,17(1):14-19.
[22]杨志坚.浙东隆起带与西南日本黑濑川构造带地质演化之比较[J].火山地质与矿产,1992,13(1):13-23.
[23]刘建华,吴健生,方银霞,等.东海陆架盆地的前新生界[J].海洋学报,2007,29(1):66-75.
[24]刘金水,廖宗廷,贾健谊,等.东海陆架盆地地质结构及构造演化[J].上海地质,2003,(3):1-5.
[25]孟宪伟,刘保华,石学法.冲绳海槽中段西陆坡下缘天然气水合物存在的可能性分析[J].沉积学报,2000,18(4):629-633.
[26]卢振权,龚建明,吴必豪,等.东海天然气水合物的地球化学标志与找矿远景[J].海洋地质与第四纪地质,2003,23(3):77-81.
[27]陶瑞明.东海西湖凹陷天然气成藏条件及分布规律[J].天然气工业,1996,16(5):10-15.
[28]叶加仁,顾惠荣.东海西湖凹陷浙东中央背斜带烃源岩生排烃史研究[J].海洋地质与第四纪地质,2001,21(8):75-80.
[29]王国纯.东海盆地油气勘探焦点问题探讨[J].中国海上油气(地质),2003,17(1):29-32.
[30]冯晓杰,蔡东升.东海陆架盆地中新生代构造演化对烃源岩分布的控制作用[J].中国海上油气(工程),2006,18(6):372-375.
[31]李纯洁,李上卿,许红.西湖凹陷中—下始新统宝石组油气地质与勘探潜力[J].海洋地质与第四纪地质,2004,24(4):81-87.
[32]闫桂京,肖国林,陈建文,等.基隆凹陷油气资源潜力[J].海洋地质与第四纪地质,2003,19(8):24-26.
[33]栾锡武,赵克斌,孙冬胜,等.鄂霍次克海天然气水合物成藏条件分析[J].海洋地质与第四纪地质,2006,26(6):91-100.
[34]Su X,Baumann K H,Thiede J.Calcareous nannofossils from leg168:Biochronology and diagenesis[M]//Fisher A,Davis E E,Escutia C.Proceedings of the Ocean Drilling Program,ScientificResults.College Station,Texas:Texas A&MUniversity(OceanDrilling Program),2000:39-49.
[35]张振国,方念乔,高莲凤,等.气体水合物在海洋中的分布及其赋存的海洋地质特征[J].资源开发与市场,2006,22(4):337-340.
[36]张光学,黄永样,祝有海,等.南海天然气水合物成矿远景[J].海洋地质与第四纪地质,2002,22(1):75-81.
[37]于兴河,张志杰,苏新,等.中国南海天然气水合物沉积成藏条件初探及其分布[J].地学前缘,2004,11(1):311-315.
[38]业治铮,张明书,潘志良.冲绳海槽晚更新世—全新世沉积物的初步研究[J].海洋地质与第四纪地质,1983,3(2):1-19.
[39]Ken Ikehara.Depositional pattern of the Okinawa Trough as re-vealed by 3.5 kHz sub-bottom profile and cored data[M]//Tsunogai S,Iseki K,Koike I,et al.Global Fluxes of Carbonand Its Related Substances in the Coastal Sea-Ocean-AtmosphereSystem.Yokohama:M&J International Yokohama Publishers,1995:26-31.
[40]李凤业,史玉兰,何丽娟.冲绳海槽晚更新世以来沉积速率的变化与沉积环境的关系[J].海洋与湖沼,1999,30(5):540-545.
[41]李培英,王永吉,刘振夏.冲绳海槽年代地层与沉积速率[J].中国科学(D辑),1999,29(1):50-55.
[42]刘振夏,Saito Y,李铁刚,等.冲绳海槽晚第四纪千年尺度的古海洋学研究[J].科学通报,1999,44(8):883-887.
[43]李西双,赵月霞,刘保华,等.冲绳海槽沉积演化的时空特征[J].海洋科学进展,2004,22(4):472-479.
[44]李军.冲绳海槽晚更新世以来沉积速率的时空差异及其控制因素[J].海洋地质与第四纪地质,2007,27(4):37-43.
[45]Ujiie H,Hatakeyama Y,Gu X X.Upward decrease of organicC/N ratios in the Okinawa Trough cores:proxy for tracing thepost-glacial retreat of the continental shore line[J].Palaeogeog-raphy,Palaeoclimatology,Palaeoecology,2001,165:129-140.
[46]李巍然,杨作升,王永吉.冲绳海槽火山岩岩石化学特征及其地质意义[J].岩石学报,1997,13(4):538-550.
[47]Wei K Y.Preface to the special section on Okinawa Trough:Sedimentary processes and paleoenvironment[J].Terrestrial,Atmospheric and Oceanic Sciences,2005,16(1):I-V.
[48]Hyndman R D,Spence G D,Chapman R,et al.Geophysicalstudies of marine gas hydrate in Northern Cascadia[J].Geo-physical Monograph Series of American Geophysical Union,2001,124:273-295.
[49]栾锡武,张训华.东海及琉球沟弧体系热流测量及分布[J].地球物理学进展,2003,18(4):670-678.
[50]栾锡武,翟世奎,干晓群.冲绳海槽中部热液活动区构造地球物理特征分析[J].沉积学报,2001,19(1):43-47.
[51]栾锡武.琉球沟弧盆系海底热流分布特征及冲绳海槽热演化的数值模拟[J].海洋与湖沼,1997,28(1):44-49.
[52]李乃胜.冲绳海槽的地质构造属性[J].海洋与湖沼,1990,21(6):536-543.
[53]李乃胜.冲绳海槽横断裂初探[J].海洋学报,1990,12(4):455-462.
[54]杨文达,张异彪,施健.冲绳海槽现代张裂特征研究[J].海洋石油,2004,24(4):15-20.
[55]栾锡武,秦蕴珊.冲绳海槽宫古段西部槽底海底气泉的发现[J].科学通报,2005,50(8):801-810.
[56]栾锡武.东海天然气水合物地震资料的识别和温、压场分析报告[R].青岛:中国科学院海洋研究所,2001:1-28.
[57]栾锡武,岳保静,鲁银涛.东海天然气水合物的地震特征[J].海洋地质与第四纪地质,2006,26(5):91-99.
[2]栾锡武,赵克斌,Obzhirov A,等.鄂霍次克海浅表层天然气水合物的勘查识别和基本特征[J].中国科学(D辑),2008,38(1):99-107.
[3]秦蕴珊,赵一阳,陈丽蓉.东海地质[M].北京:科学出版社,1987.
[4]金翔龙.东海海洋地质[M].北京:海洋出版社,1992.
[5]许东禹.中国东海地质[M].北京:地震出版社,1997.
[6]贾健谊,顾惠荣.东海西湖凹陷含油气系统与油气资源评价[M].北京:地质出版社,2002:204.
[7]李巍然,杨作升,王琦,等.冲绳海槽陆源碎屑峡谷通道搬运与海底扇沉积[J].海洋与湖沼,2001,32(4):371-380.
[8]栾锡武,高金耀,梁瑞才,等.冲绳海槽宫古段中央地堑的形态与分布[J].地质学报,2006,80(8):1149-1155.
[9]栾锡武,岳保静.冲绳海槽宫古段中央地堑中的火山分布及地质意义[J].海洋与湖沼,2007,38(3):266-271.
[10]栾锡武,秦蕴珊,张训华,等.东海陆坡及相邻槽底天然气水合物的稳定域分析[J].地球物理学报,2003,46(4):467-475.
[11]赵一阳,何丽娟,张秀莲.冲绳海槽沉积物地球化学的基本特征[J].海洋与湖沼,1984,15(4):371-379.
[12]吴明清,王贤觉.东海沉积物的稀土和微量元素[J].地球化学,1991,20(1):40-46.
[13]杜德文,孟宪伟,王永吉.沉积物物源组成的定量判识方法及其在冲绳海槽的应用[J].海洋与湖沼,1999,30(6):532-539.
[14]苟淑名.冲绳海槽表层沉积物孢粉组合特征[J].海洋科学,1982,6:14-18.
[15]李凡,张秀荣,李永植.南黄海埋藏古三角洲[J].地理学报,1998,53(3):238-244.
[16]谢钦春,叶银灿,陆炳火.东海陆架坡折地形和沉积作用过程[J].海洋学报,1984,6(1):61-71.
[17]茅志昌,李九发,吴华林.上海市滩涂促淤圈围研究[J].泥沙研究,2003,(2):77-81.
[18]任美锷.黄河的输沙量:过去、现在和将来——距今15万年以来的黄河泥沙收支表[J].地球科学进展,2006,21(6):551-563.
[19]戴仕宝,杨世伦,蔡爱民.51年来珠江流域输沙量的变化[J].地理学报,2007,62(5):545-554.
[20]蒋富清,李安春,李铁刚.冲绳海槽北端表层沉积物过渡元素地球化学特征[J].海洋与湖沼,2006,37(1):75-83.
[21]赵金海,唐建,薄玉玲.关于东海新生代盆地油气勘探的若干见解[J].中国海上油气(地质),2003,17(1):14-19.
[22]杨志坚.浙东隆起带与西南日本黑濑川构造带地质演化之比较[J].火山地质与矿产,1992,13(1):13-23.
[23]刘建华,吴健生,方银霞,等.东海陆架盆地的前新生界[J].海洋学报,2007,29(1):66-75.
[24]刘金水,廖宗廷,贾健谊,等.东海陆架盆地地质结构及构造演化[J].上海地质,2003,(3):1-5.
[25]孟宪伟,刘保华,石学法.冲绳海槽中段西陆坡下缘天然气水合物存在的可能性分析[J].沉积学报,2000,18(4):629-633.
[26]卢振权,龚建明,吴必豪,等.东海天然气水合物的地球化学标志与找矿远景[J].海洋地质与第四纪地质,2003,23(3):77-81.
[27]陶瑞明.东海西湖凹陷天然气成藏条件及分布规律[J].天然气工业,1996,16(5):10-15.
[28]叶加仁,顾惠荣.东海西湖凹陷浙东中央背斜带烃源岩生排烃史研究[J].海洋地质与第四纪地质,2001,21(8):75-80.
[29]王国纯.东海盆地油气勘探焦点问题探讨[J].中国海上油气(地质),2003,17(1):29-32.
[30]冯晓杰,蔡东升.东海陆架盆地中新生代构造演化对烃源岩分布的控制作用[J].中国海上油气(工程),2006,18(6):372-375.
[31]李纯洁,李上卿,许红.西湖凹陷中—下始新统宝石组油气地质与勘探潜力[J].海洋地质与第四纪地质,2004,24(4):81-87.
[32]闫桂京,肖国林,陈建文,等.基隆凹陷油气资源潜力[J].海洋地质与第四纪地质,2003,19(8):24-26.
[33]栾锡武,赵克斌,孙冬胜,等.鄂霍次克海天然气水合物成藏条件分析[J].海洋地质与第四纪地质,2006,26(6):91-100.
[34]Su X,Baumann K H,Thiede J.Calcareous nannofossils from leg168:Biochronology and diagenesis[M]//Fisher A,Davis E E,Escutia C.Proceedings of the Ocean Drilling Program,ScientificResults.College Station,Texas:Texas A&MUniversity(OceanDrilling Program),2000:39-49.
[35]张振国,方念乔,高莲凤,等.气体水合物在海洋中的分布及其赋存的海洋地质特征[J].资源开发与市场,2006,22(4):337-340.
[36]张光学,黄永样,祝有海,等.南海天然气水合物成矿远景[J].海洋地质与第四纪地质,2002,22(1):75-81.
[37]于兴河,张志杰,苏新,等.中国南海天然气水合物沉积成藏条件初探及其分布[J].地学前缘,2004,11(1):311-315.
[38]业治铮,张明书,潘志良.冲绳海槽晚更新世—全新世沉积物的初步研究[J].海洋地质与第四纪地质,1983,3(2):1-19.
[39]Ken Ikehara.Depositional pattern of the Okinawa Trough as re-vealed by 3.5 kHz sub-bottom profile and cored data[M]//Tsunogai S,Iseki K,Koike I,et al.Global Fluxes of Carbonand Its Related Substances in the Coastal Sea-Ocean-AtmosphereSystem.Yokohama:M&J International Yokohama Publishers,1995:26-31.
[40]李凤业,史玉兰,何丽娟.冲绳海槽晚更新世以来沉积速率的变化与沉积环境的关系[J].海洋与湖沼,1999,30(5):540-545.
[41]李培英,王永吉,刘振夏.冲绳海槽年代地层与沉积速率[J].中国科学(D辑),1999,29(1):50-55.
[42]刘振夏,Saito Y,李铁刚,等.冲绳海槽晚第四纪千年尺度的古海洋学研究[J].科学通报,1999,44(8):883-887.
[43]李西双,赵月霞,刘保华,等.冲绳海槽沉积演化的时空特征[J].海洋科学进展,2004,22(4):472-479.
[44]李军.冲绳海槽晚更新世以来沉积速率的时空差异及其控制因素[J].海洋地质与第四纪地质,2007,27(4):37-43.
[45]Ujiie H,Hatakeyama Y,Gu X X.Upward decrease of organicC/N ratios in the Okinawa Trough cores:proxy for tracing thepost-glacial retreat of the continental shore line[J].Palaeogeog-raphy,Palaeoclimatology,Palaeoecology,2001,165:129-140.
[46]李巍然,杨作升,王永吉.冲绳海槽火山岩岩石化学特征及其地质意义[J].岩石学报,1997,13(4):538-550.
[47]Wei K Y.Preface to the special section on Okinawa Trough:Sedimentary processes and paleoenvironment[J].Terrestrial,Atmospheric and Oceanic Sciences,2005,16(1):I-V.
[48]Hyndman R D,Spence G D,Chapman R,et al.Geophysicalstudies of marine gas hydrate in Northern Cascadia[J].Geo-physical Monograph Series of American Geophysical Union,2001,124:273-295.
[49]栾锡武,张训华.东海及琉球沟弧体系热流测量及分布[J].地球物理学进展,2003,18(4):670-678.
[50]栾锡武,翟世奎,干晓群.冲绳海槽中部热液活动区构造地球物理特征分析[J].沉积学报,2001,19(1):43-47.
[51]栾锡武.琉球沟弧盆系海底热流分布特征及冲绳海槽热演化的数值模拟[J].海洋与湖沼,1997,28(1):44-49.
[52]李乃胜.冲绳海槽的地质构造属性[J].海洋与湖沼,1990,21(6):536-543.
[53]李乃胜.冲绳海槽横断裂初探[J].海洋学报,1990,12(4):455-462.
[54]杨文达,张异彪,施健.冲绳海槽现代张裂特征研究[J].海洋石油,2004,24(4):15-20.
[55]栾锡武,秦蕴珊.冲绳海槽宫古段西部槽底海底气泉的发现[J].科学通报,2005,50(8):801-810.
[56]栾锡武.东海天然气水合物地震资料的识别和温、压场分析报告[R].青岛:中国科学院海洋研究所,2001:1-28.
[57]栾锡武,岳保静,鲁银涛.东海天然气水合物的地震特征[J].海洋地质与第四纪地质,2006,26(5):91-99.
版权所有：© 2023 中国地质图书馆 中国地质调查局地学文献中心