东海陆架两期沙脊的时空对比
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摘要
基于高分辨率的单道地震和多波束测深数据,识别并对比了东海陆架中部同一海区相距20余万年的层U14和层U2两期沙脊群,其中层U14期沙脊属于埋藏沙脊,位于东海海底以下90 m深处,推测属于距今320~200 ka的海侵体系域(TST),沙脊顶界面是该期海侵的最大洪泛面(MFS);层U2期沙脊位于东海陆架,属于衰退沙脊,系末次盛冰期(LGM)以来的TST,顶界面是LGM以来的MFS。尽管两期沙脊形成年代相距20余万年,地层层位相距近90 m,但是沙脊群总体走向一致,表明距今2×105a以来东海陆架潮波基本格局稳定。从层U2期可识别出4个亚期沙脊,通过多波束海底地形图可识别出4组走向的沙脊,多亚期、多走向沙脊是LGM以来海平面阶梯状波动在海底地形演变过程中的响应证据。
On the basis of the high-resolution single-channel sparker seismic profiles and MBES(multi-beam echo sounding),the LSRs(linear sand ridges) on Stratum U2 and Stratum U14 on the ECS(East China Sea) shelf are identified and contrasted each other,their form ages are different,more than 200 ka.The sand ridges on Stratum U14 which is bellow seafloor 90 m are buried sand ridges,and belong to TST(transgressive systems tract) of 320~200 ka BP,and the upper bounding surfaces of the sand ridge units are therefore considered as the MFS(maximum flooding surface) of this transgressive.The sand ridges on Stratum U2 are recessive sand ridges,which have belonged to the TST since the LGM(last glacial maximum),and their upper bounding surfaces are the MFS of the LGM.Although the form ages of two sand ridge units are different,more than 200 ka,and their stratigraphy positions are different,more than 90 m,the general strikes of sand ridges are similar.It is suggested that the palaeo-tidal components of the ECS have been steady since 200 ka.Four substages sand ridges are identified from the stratigraphy of Stratum U2,and four trends of sand ridges are distinguished from the topographic map of the MBES too.These multistages and multitrend sand ridges are the evidences that the evolution of submarine topography of the ECS has met the response of sea-level stepped changes since the LGM.
On the basis of the high-resolution single-channel sparker seismic profiles and MBES(multi-beam echo sounding),the LSRs(linear sand ridges) on Stratum U2 and Stratum U14 on the ECS(East China Sea) shelf are identified and contrasted each other,their form ages are different,more than 200 ka.The sand ridges on Stratum U14 which is bellow seafloor 90 m are buried sand ridges,and belong to TST(transgressive systems tract) of 320~200 ka BP,and the upper bounding surfaces of the sand ridge units are therefore considered as the MFS(maximum flooding surface) of this transgressive.The sand ridges on Stratum U2 are recessive sand ridges,which have belonged to the TST since the LGM(last glacial maximum),and their upper bounding surfaces are the MFS of the LGM.Although the form ages of two sand ridge units are different,more than 200 ka,and their stratigraphy positions are different,more than 90 m,the general strikes of sand ridges are similar.It is suggested that the palaeo-tidal components of the ECS have been steady since 200 ka.Four substages sand ridges are identified from the stratigraphy of Stratum U2,and four trends of sand ridges are distinguished from the topographic map of the MBES too.These multistages and multitrend sand ridges are the evidences that the evolution of submarine topography of the ECS has met the response of sea-level stepped changes since the LGM.
引文
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[23]SCOURSE J,UEHARA K,WAINWRIGHT A.Celtic Sea linear tidal sand ridges,the Irish Sea ice stream and the Fleuve Manche:palaeotidal modelling of a transitional passive margin depositional system[J].Mar Geol,2009,doi:10.1016/j.margeo.2008.12.010.
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[28]LI M Z,KING E L.Multibeam bathymetric investigations of the morphology of sand ridges and associated bedforms and their relationto storm processes,Sable Island Bank,Scotian Shelf[J].Mar Geol,2007,243:200—228.
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[32]LIU J P,LI A C,XU K H,et al.Sedimentary features of the Yangtze River-derived along-shelf clinoform deposit in the East China Sea[J].Cont Shelf Res,2006,26:2141—2156.
[33]LIU J P,MILLIMAN J D,GAO S,et al.Holocene development of the Yellow River’s subaqueous delta,North Yellow Sea[J].MarGeol,2004,209:45—67.
[34]FAIRBANKS R G.A 17 000-year galcio-eustatic sea level record:influence of glacial melting rates on the Younger Dryas event anddeep-ocean circulation[J].Nature,1989,342:637—642.
[35]HUTHNANCE J M.On one mechanism forming liner sand banks[J].Estuar Coast Shelf Sci,1982,14:79—99.
[36]杨子赓,王圣洁,张光威,等.冰消期海侵进程中南黄海潮流沙脊的演化模式[J].海洋地质与第四纪地质,2001,21(3):1—10.
[2]刘光鼎.中国海区及邻域地质地球物理系列图(1/500万)[Q].北京:地质出版社,1992.
[3]WU Z Y,JIN X L,LI J B,et al.Linear sand ridges on the outer shelf of the East China Sea[J].Chin Sci Bull,2005,50(21):2517—2528.
[4]朱永其,曾成开,冯韵.东海陆架地貌特征[J].东海海洋,1984,2(2):1—13.
[5]YANG C S.Active moribund and buried tidal sand ridges in the East China Sea and the southern Yellow Sea[J].Mar Geol,1989,88:97—116.
[6]杨文达.东海海底沙脊的结构及沉积环境[J].海洋地质与第四纪地质,2002,22(1):9—16.
[7]刘振夏.对东海扬子浅滩成因的再认识[J].海洋学报,1996,18(2):85—92.
[8]叶银灿,庄振业,来向华,等.东海扬子浅滩砂质底形研究[J].中国海洋大学学报,2004,34(6):1057—1062.
[9]SAITO Y,KATAYAMA H,IKEHARA K,et al.Transgressive and highstand systems tracts and post-glacial transgression,the EastChina Sea[J].Sediment Geol,1998,122:217—232.
[10]YOO D G,LEE C W,MIN G H,et al.Late Quaternary seismic stratigraphy and sedimentation of the southeastern continental shelf,Korea Strait[J].Mulli-Tamsa,2005,8(3):201—206.
[11]CHEN Z Y,SAITO Y,HORI K,et al.Early Holocene mud-ridge formation in the Yangtze offshore,China:a tidal-controlled estuar-ine pattern and sea-level implications[J].Mar Geol,2003,198:245—257.
[12]刘忠臣,陈义兰,丁继胜,等.东海海底地形分区特征和成因研究[J].海洋科学进展,2003,21(2):160—173.
[13]李广雪,杨子赓,刘勇.中国东部海域海底沉积环境成因研究[M].北京:科学出版社,2004:1—44.
[14]LIAO H R,YU H S,SU C C.Morphology and sedimentation of sand bodies in the tidal shelf sea of eastern Taiwan Strait[J].Mar Ge-ol,2008,248:161—178.
[15]唐保根.东海陆架第四纪地层[M]//杨子赓,林和茂.中国第四纪地层与国际对比.北京:地质出版社,1996:56—75.
[16]BERNéS,VAGNER P.Pleistocene forced regressions and tidal sand ridges in the East China Sea[J].Mar Geol,2002,188:293—315.
[17]刘振夏,夏东兴.中国近海潮流沉积沙体[M].北京:海洋出版社,2004.
[18]LIU Z X,BERNE S,SAITO Y,et al.Internal architecture and mobility of tidal sand ridges in the East China Sea[J].Cont Shelf Res,2007,27(13):1820—1834.
[19]印萍.东海陆架冰后期潮流沙脊地貌与内部结构特征[J].海洋科学进展,2003,21(2):181—187.
[20]吴自银,金翔龙,李家彪.中更新世以来长江口至冲绳海槽高分辨率地震地层学研究[J].海洋地质与第四纪地质,2002,22(2):9—20.
[21]UEHARA K,SAITO Y,HORI K.Paleotidal regime in the Changjiang(Yangtze)Estuary,the East China Sea,and the Yellow Sea at6 ka and 10 ka estimated from a numerical model[J].Mar Geol,2002,183:179—192.
[22]UEHARA K,SAITO Y.Late Quaternary evolution of the Yellow/East China Sea tidal regime and its impacts on sediments dispersaland seafloor morphology[J].Sediment Geol,2003,162:25—38.
[23]SCOURSE J,UEHARA K,WAINWRIGHT A.Celtic Sea linear tidal sand ridges,the Irish Sea ice stream and the Fleuve Manche:palaeotidal modelling of a transitional passive margin depositional system[J].Mar Geol,2009,doi:10.1016/j.margeo.2008.12.010.
[24]TODD B J,GORDON B J F,ROBERT C,et al.Quaternary geology and surficial sediment processes,Browns Bank,Scotian Shelf,based on multibeam bathymetry[J].Mar Geol,1999,162:165—214.
[25]GOFF J A,SWIFT D J P,DUNCAN C S,et al.High-resolution swath sonar investigation of sand ridge,dune and ribbon morphologyin the offshore environment of the New Jersey margin[J].Mar Geol,1999,161:307—337.
[26]GOFF J A,KRAFTC B J,MAYER L A,et al.Seabed characterization on the New Jersey middle and outer shelf:correlatability andspatial variability of seafloor sediment properties[J].Mar Geol,2004,209:147—172.
[27]GOFF J A,AUSTIN J A,GULICK S,et al.Recent and modern marine erosion on the New Jersey outer shelf[J].Mar Geol,2005,216:275—296.
[28]LI M Z,KING E L.Multibeam bathymetric investigations of the morphology of sand ridges and associated bedforms and their relationto storm processes,Sable Island Bank,Scotian Shelf[J].Mar Geol,2007,243:200—228.
[29]KENNETT J.海洋地质学[M].成国栋,谢继哲,许东禹等译.北京:海洋出版社,1992:522.
[30]MARTINSON D G,PISIAS N G,HAYS J D,et al.Age dating and the orbital theory of the ice ages:development of a high-resolution0 to 300 000 year chronostratigraphy[J].Quat Res,1987,27:1—29.
[31]SKENE K I,PIPER D J W,AKSU A E,et al.Evaluation of the global oxygen isotope curve as a proxy for Quaternary sea level bymodeling of delta progradation[J].J Sediment Res,1998,68:1077—1092.
[32]LIU J P,LI A C,XU K H,et al.Sedimentary features of the Yangtze River-derived along-shelf clinoform deposit in the East China Sea[J].Cont Shelf Res,2006,26:2141—2156.
[33]LIU J P,MILLIMAN J D,GAO S,et al.Holocene development of the Yellow River’s subaqueous delta,North Yellow Sea[J].MarGeol,2004,209:45—67.
[34]FAIRBANKS R G.A 17 000-year galcio-eustatic sea level record:influence of glacial melting rates on the Younger Dryas event anddeep-ocean circulation[J].Nature,1989,342:637—642.
[35]HUTHNANCE J M.On one mechanism forming liner sand banks[J].Estuar Coast Shelf Sci,1982,14:79—99.
[36]杨子赓,王圣洁,张光威,等.冰消期海侵进程中南黄海潮流沙脊的演化模式[J].海洋地质与第四纪地质,2001,21(3):1—10.
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