南海北部大陆架莺琼盆地新生代海平面变化
|
摘要
南海北部大陆架莺琼盆地是建立西太平洋新生代海平面变化的关键地区之一。基于有孔虫和钙质超微化石资料所建立的莺歌海盆地和琼东南盆地新生代相对分辨率较高的年代地层格架,通过南海海域表层建立的浮游有孔虫含量与水深的定量关系,辅以古生态、成因相及特征沉积构造分析和反射地震剖面的海岸上超分析,编制了海平面变化曲线。识别出包含三个完整二级海平面变化旋回和半周期的海平面上升旋回。海平面变化幅度在0～200 m之间。海水最深的时期在早中新世晚期至中中新世早期以及上新世早期,与Haq曲线较为吻合。
The Yinggehai-Qiongdongnan(Ying-Qiong) Basin is a part of the South China Sea Shelf Basin.It is the key area to set up the Cenozoic sea level change cycles in west Pacific Ocean.Based on a relative high-resolution chronostratigraphic framework which formed from the data of foraminifera and Calcareous nannofossils,the curves of Cenozoic sea level changes in Ying-Qiong Basin was reconstructed according to the quantitative relationship between the percentage of pelagic foraminifera and water depth in the surface layer of South China Sea and by the analysis of the paleoecology,the geneses phase,the characteristics of sedimentary structures and the coastal onlap recognized in seismic reflection profiles.Three integrated 2nd-graded cycles of sea level changes and a half period cycle of sea level rising was set up from Oligocene to nowadays.The sea-level changes ranged between 0m and 200m.The deepest water appeared from the late Early Miocene to the early Middle Miocene.Compared with the Haq's curve(1988),the curves are similar in long-term and high order cycle of sea level changes.Xie Jinyou,Zhu Youhua,Li Xushen,Mai Wen,Zhao Pengxiao
The Yinggehai-Qiongdongnan(Ying-Qiong) Basin is a part of the South China Sea Shelf Basin.It is the key area to set up the Cenozoic sea level change cycles in west Pacific Ocean.Based on a relative high-resolution chronostratigraphic framework which formed from the data of foraminifera and Calcareous nannofossils,the curves of Cenozoic sea level changes in Ying-Qiong Basin was reconstructed according to the quantitative relationship between the percentage of pelagic foraminifera and water depth in the surface layer of South China Sea and by the analysis of the paleoecology,the geneses phase,the characteristics of sedimentary structures and the coastal onlap recognized in seismic reflection profiles.Three integrated 2nd-graded cycles of sea level changes and a half period cycle of sea level rising was set up from Oligocene to nowadays.The sea-level changes ranged between 0m and 200m.The deepest water appeared from the late Early Miocene to the early Middle Miocene.Compared with the Haq's curve(1988),the curves are similar in long-term and high order cycle of sea level changes.Xie Jinyou,Zhu Youhua,Li Xushen,Mai Wen,Zhao Pengxiao
引文
[1]Haq B U,Hardenbol J,Vail P R.Mesozoic and Cenozoic chronostratigraphy and eustatic cycles[J].Society of Economic Paleontologist and Special Publication,USA,1988(42):71-108.
[2]武法东,李思田,陆永潮,等.东海陆架盆地第三纪海平面变化[J].地质科学,1998,33(2):214-221.
[3]郝诒纯,陈平富,万晓樵,等.南海莺歌海—琼东南盆地晚第三纪层序地层与海平面变化[J].现代地质,2000,14(3):237-245.
[4]董军社,陈平富,万晓樵,等.南海北部崖19-1-1井晚第三纪有孔虫动物群演替与古水深变化[J].现代地质,2000,14(3):291-294.
[5]何卫军,谢金有,刘新宇,等.莺歌海盆地DF1-1-11井有孔虫生物地层与沉积环境研究[J].地层学杂志,2011,35(1):81-87.
[6]陈中强,钟石兰,杨少坤,等.微古生物在高分辨层序地层学中的应用——以珠江口盆地惠州凹陷层序地层分析为例[J].微体古生物学报,1998,15(2):134-143.
[7]李学杰,陈芳,陈超云,等.南海西部浮游有孔虫含量与水深关系定量研究[J].古地理学报,2004,6(4):442-447.
[8]刘新宇,谢金有,张伙兰,等.南海北部莺琼盆地浮游有孔虫年代地层研究[J].微体古生物学报,2009,26(2):181-192.
[9]谢金有,祝幼华,麦文,等.南海北部莺琼盆地钙质超微化石年代地层[J].微体古生物学报,2010,27(4):289-298.
[10]Blow W H.Late middle Eocene to recent planktonic forminiferal biostratigraphy[M]//Bronnimann P,Renz H H,eds.Proceedings of the first international conference planktonic microfossils,Geneva,1967.Leiden:Brill/Netherlans,1969.
[11]Blow W H.The Cainozoic globigerinida[M].Brill Leiden,1979,3:1-1413.
[12]Bolli H M,Saunders J B.Oligocene to Holocene low latitude planktic foraminifera[M]//Bolli H M,et al,eds.Planktonic Stratigraphy.Cambridge:Cambridge University Press,1985.
[13]Martini E.Standard Tertiary and Quaternary calcareous nanno-plankton zonation[C]//Farinacci A,eds.Proceedings of the II planktonic conference,Roma,1970Roma:Teknoscienza1971:739-785.
[14]Okada H,Bukry D.Supplementary modification and intro-duction of code numbers to the low-latitude coccolith biostigrphic zonation[J].Marine Micropaleontology,1980,5(3):321-325.
[15]汪品先,赵鸿泉,翦知湣,等.南海三千万年的深海记录[J].科学通报,2003,48(21):2206-2215.
[16]李前裕,Lucas Lourens,汪品先,等.新近纪海相生物地层事件年龄新编[J].地层学杂志,2007,31(3):197-208.
[17]Gradstein F M,Ogg J G,Smith A G.A geologic time scale[M].Cambridge:Cambridge University Press,2004.
[18]Vail P R,Mitchum R M,Todd R B Jr,et al.Seismic stratig-raphy and global changes of sea level[J].AAPG,Memoir 1977,26:49-212.
[19]Harris P M,Frost S H,Seiglie G A,et al.Regional unconfor-mities and depositional cycles,Cretaceous of the Arabian peninsula[J].AAPG Memoir,1984,36:67-80.
[20]钱建兴.南海8KL岩芯氧同位素记录与海平面变化[J].地质学报,1994(4):369-387.
[21]Kendall C G St C,Lerche I.The Rise and fall of eustasy[J].Society of Economic Paleontologist and Special Publication USA,1988,(42):3-18.
[22]秦国权.珠江口盆地新生代晚期层序地层划分和海平面变化[J].中国海上油气,2002,16(1):1-18.
[23]黄虑生.珠江口盆地渐新统—上新统高分辨率生物地层学研究[J].海相油气地质,1996,1(4):13-20.
[2]武法东,李思田,陆永潮,等.东海陆架盆地第三纪海平面变化[J].地质科学,1998,33(2):214-221.
[3]郝诒纯,陈平富,万晓樵,等.南海莺歌海—琼东南盆地晚第三纪层序地层与海平面变化[J].现代地质,2000,14(3):237-245.
[4]董军社,陈平富,万晓樵,等.南海北部崖19-1-1井晚第三纪有孔虫动物群演替与古水深变化[J].现代地质,2000,14(3):291-294.
[5]何卫军,谢金有,刘新宇,等.莺歌海盆地DF1-1-11井有孔虫生物地层与沉积环境研究[J].地层学杂志,2011,35(1):81-87.
[6]陈中强,钟石兰,杨少坤,等.微古生物在高分辨层序地层学中的应用——以珠江口盆地惠州凹陷层序地层分析为例[J].微体古生物学报,1998,15(2):134-143.
[7]李学杰,陈芳,陈超云,等.南海西部浮游有孔虫含量与水深关系定量研究[J].古地理学报,2004,6(4):442-447.
[8]刘新宇,谢金有,张伙兰,等.南海北部莺琼盆地浮游有孔虫年代地层研究[J].微体古生物学报,2009,26(2):181-192.
[9]谢金有,祝幼华,麦文,等.南海北部莺琼盆地钙质超微化石年代地层[J].微体古生物学报,2010,27(4):289-298.
[10]Blow W H.Late middle Eocene to recent planktonic forminiferal biostratigraphy[M]//Bronnimann P,Renz H H,eds.Proceedings of the first international conference planktonic microfossils,Geneva,1967.Leiden:Brill/Netherlans,1969.
[11]Blow W H.The Cainozoic globigerinida[M].Brill Leiden,1979,3:1-1413.
[12]Bolli H M,Saunders J B.Oligocene to Holocene low latitude planktic foraminifera[M]//Bolli H M,et al,eds.Planktonic Stratigraphy.Cambridge:Cambridge University Press,1985.
[13]Martini E.Standard Tertiary and Quaternary calcareous nanno-plankton zonation[C]//Farinacci A,eds.Proceedings of the II planktonic conference,Roma,1970Roma:Teknoscienza1971:739-785.
[14]Okada H,Bukry D.Supplementary modification and intro-duction of code numbers to the low-latitude coccolith biostigrphic zonation[J].Marine Micropaleontology,1980,5(3):321-325.
[15]汪品先,赵鸿泉,翦知湣,等.南海三千万年的深海记录[J].科学通报,2003,48(21):2206-2215.
[16]李前裕,Lucas Lourens,汪品先,等.新近纪海相生物地层事件年龄新编[J].地层学杂志,2007,31(3):197-208.
[17]Gradstein F M,Ogg J G,Smith A G.A geologic time scale[M].Cambridge:Cambridge University Press,2004.
[18]Vail P R,Mitchum R M,Todd R B Jr,et al.Seismic stratig-raphy and global changes of sea level[J].AAPG,Memoir 1977,26:49-212.
[19]Harris P M,Frost S H,Seiglie G A,et al.Regional unconfor-mities and depositional cycles,Cretaceous of the Arabian peninsula[J].AAPG Memoir,1984,36:67-80.
[20]钱建兴.南海8KL岩芯氧同位素记录与海平面变化[J].地质学报,1994(4):369-387.
[21]Kendall C G St C,Lerche I.The Rise and fall of eustasy[J].Society of Economic Paleontologist and Special Publication USA,1988,(42):3-18.
[22]秦国权.珠江口盆地新生代晚期层序地层划分和海平面变化[J].中国海上油气,2002,16(1):1-18.
[23]黄虑生.珠江口盆地渐新统—上新统高分辨率生物地层学研究[J].海相油气地质,1996,1(4):13-20.
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