琼东南盆地层序地层和深水区沉积充填特征
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摘要
南海是我国也是西太平洋西部的一个巨大边缘海,北面靠近华南大陆边缘、西面邻接印支陆块、南面靠近加里曼丹岛、东面与马尼拉海沟为界,位于太平洋板块、印一澳板块和欧亚板块三大板块交汇的位置。由于西太平洋板块、欧亚板块和印度板块俯冲碰撞相互作用,以及巴拉望和礼乐滩等微陆块与加里曼丹岛挤压聚敛等构造活动,渐形成南海目前的构造格局：即北部边缘为被动陆缘,东部边缘为俯冲消亡带,西缘以走滑剪切,南缘以聚敛边缘为特征。南海自中中新世三亚组(16.7Ma)停止扩张,在扩张过程中,产生了许多沉积盆地,盆地内沉积了大量的来自于陆源的富含有机质物质,形成了良好的生、运、储等石油地质条件,因此南海成为我国深水油气资源勘探开发的首选最佳远景区。
琼东南盆地位于南海北部大陆边缘,是新生代形成的断陷盆地。其构造演化上的特征为“下断上坳”,以破裂不整合面T60为界,经历了古近纪裂陷阶段和新近纪的裂后热沉降阶段。根据断裂发育情况以及盆地充填变形特征,将裂陷和裂后两大演化阶段进一步细分为4个构造幕,分别是裂陷Ⅰ幕(始新世-早渐新世断陷期)、裂陷Ⅱ幕(晚渐新世断坳期)、裂后Ⅰ幕(早-中中新世热沉降期)和裂后Ⅱ幕(晚中新世-第四纪加速沉降期)。
本文以国家科技重大专项—“南海北部深水区潜在富生烃凹陷评价”中的子课题“南海北部深水区古气候和古环境研究”(2011ZX05025-002-03)为依托,以琼东南盆地深水区油气钻井LS33-1-1井和LS22-1-1井及贯穿琼东南盆地的十几条地震剖面为研究对象,通过地震与古生物地层标定,结合测井与沉积物粒度分析,建立了琼东南盆地等时层序地层格架,探讨了琼东南盆地沉积相和深水区沉积充填特征,为今后琼东南盆地石油勘探奠定了基础。论文主要成果包括：
(1)通过地震地层和古生物地层标定,建立了LS22-1-1井和LS33-1-1井两口深水探井的年代地层框架。主要的地层单元包括：始新统岭头组,渐新统崖城组和陵水组,中新统三亚组、梅山组和黄流组,上新统莺歌海组,地层的地震界面分别为T100(始新统底界)、T80(32Ma)、T70(28.4Ma)、T60(23Ma)、T50(16.OMa)、T40(11.6Ma)、T30(5.5Ma)和T20(1.8Ma)。在32～1.8Ma的地层中,共识别出一级层序界面1个(T60),二级层序界面6个(分别是T100、T80、T70、T60、T40、T20)。以T60为界将地层分割为两个一级层序。以T100(始新统底)、T80(始新统顶)、T70(崖城组顶)、T60(陵水组顶)、T40(梅山组顶)、T20(莺歌海组顶)为界,将地层分割为5个二级层序。建立了包含18个三级层序的琼东南盆地的层序地层格架。划分出T60-T20各三级层序内的低位体系域、海进体系域和高位体系域共28个
(2)通过LS33-1-1和LS22-1-1两口深水探井古生物资料,利用生物化石(主要为浮游有孔虫和钙质超微化石)基准面的年龄值,确定钻孔中年龄与深度的对应关系,建立了生物年代序列和等时层序地层格架,为油气地质条件分析和古环境恢复奠定了基础。
(3)根据陆坡体系的外部形态及其内部沉积构成特征,在空间上自西向东可以将其划分为为4类：进积型陆坡、滑塌型陆坡、水道化型陆坡和宽缓单斜型陆坡。在陆坡上发育了：陆坡峡谷、浊流沉积、滑塌沉积、碎屑流沉积、滑移沉积和沉积物波等沉积类型。
(4)琼东南盆地中央峡谷呈北东向展布,平面形态呈“S”型；西段起源于莺歌海盆地中部,向东经乐东、陵水、松涛、宝岛、长昌5大凹陷,最后延伸进入西沙海槽。在中央峡谷充填了块体流、天然堤及漫溢沉积、深海泥质沉积、浊积水道、浊积席状砂等沉积微相。峡谷西段的乐东凹陷和陵水凹陷的西部以浊积水道沉积为主,东段为浊积水道与块体流沉积互层沉积,浊积水道和浊积席状砂是深水区油气勘探的主要储层类型。
(5)通过对琼东南盆地LS22-1-1井、LS33-1-1井岭头组、崖城组、陵水组、三亚组、梅山组和黄流组和莺歌海组地层的粒度资料分析,结果表明从始新世岭头组到上新世莺歌海组,沉积物的平均粒径总体上呈减小的趋势。盆地的沉积环境经历了湖相、滨岸相、陆表海相向浅海-半深海环境的演变,水动力条件从强到弱。
The South China Sea is a huge marginal sea at the western Pacific.The boundary of north is China continental margin;The boundary of west is near the Yinzhi continent;The boundary of south is near Kalimantan island;The boundary of east is near Marnila trench.The South China Sea is located in convergence parts of the Pacific plate、Indian-Australian plate and Eurasian plate.For the reason of subducting the Pacific plate to Eurasian plate,collision orogeny Indian-Australian plate to Eurasian plat, covergence Palawan and ReedBank to Kalimantan island. These tectonic activity cause the present tectonic framework of the South China Sea:the north is passive continental margin,the east is subduction belt, the south is covergence belt, the west is strike-slip shearing belt.The South China Sea stopped expanding from the end of the early Miocene(16.7Ma). During the expansion process, The South China Sea developed a wide range of depositional basin, which received a large amount of land-sourced material,riching in organic matter, and had good hydrocarbon source rock, transporting and storage of petroleum geological conditions. The deep water hydrocarbon prospective areas in the Northern South China Sea become the consensus of the international community.
The Qingdongnan basin is located in the Northern South China Sea, which is a graben basin during Cenozoic. Its bottom half is graben basin, the top half is sag basin. The boundary between two half is seismic interface T60. Throughout the period of geological history, the South China Sea has main undergone rift epoch from Paleocene to early Oligocene, Rift fault-depression-squeeze reversed in late Oligocene and the sedimentation period from the early Pliocene to Quaternary.
This paper is based on major national technology special project "The research on The evaluation about the potential rich hydrocarbon Sag in deepwater area of Northern South China Sea"-branch project:"The research of paleoenvironment and paleoclimate in deepwater area of Northern South China Sea"(2011ZX05025-002-03), basing on the paleontology information of the oil and gas well LS22-1-1、LS33-1-1and more than ten seismic profile. Analysing of the LS22-1-1、LS33-1-1well about the seismic interface icons of palaeontogical fossils data, log information, grain size of sediment, and then giving isochron sequence stratigraphic framework, analysis the sedimentary facies and depositional characteristics of deepwater area in Qingdongnan basin, give help to oilexploration in the future. The main conclusions are as follows:
(1) Analysing of the LS33-1-1and LS22-1-1well about the seismic interface icons of palaeontological fossils data, and then giving paleontological stratigraphic division for the two wells. The main stratigraphic formation includes:eocene-lingtou formation; oligocene-yacheng and lingshui formation; miocene-sanya、meishan and huangliu formation; pliocene-yinggehai formation. The seismic interfaces are respectively T100、T80(32Ma)、T70(28.4)、T60(23.0Ma)、T50(16.0Ma) T40(11.6Ma)、T30(5.5Ma)、T20(1.8Ma). During32-1.8Ma, we recognise1primary sequence interface(T60),6sencondary sequence interface(T100、T80、T70、T60、 T50、T40、T30、T20), including2primary sequences、5sencondary sequences and18tertiary sequence stratigraphy, we recognise28low stand tract, transgressive stand tract and high stand tract.
(2) Quantitative bio stratigraphic analysis methods were used to study the paleontological data of the LS33-1-1and LS22-1-1well, we determine the sequence interface age and the corresponding relation of age and depth,establish the biological sequence and isochronal sequence stratigraphic framework.
(3) According to the slope system external form and its internal deposit formation, which can be divided into4classes from the west to the east:progradation slope, slumping slope, Channel change slope and Rolling monoclinic slope. Sedimentation type includes:Slope canyon、turbid flow、slumping、debris flow、slide and sediment waves.
(4) The central valley is "s" type in the plane, extended direction NE. Originating from yinggehai basin to xisha trough,the central valley goes through ledong sag,lingshui sag, songtao sag, baodao sag and changchang sag.The sedimentary facies in The central valley includes5types,such as:turbidity channel, turbidite sand sheet,natural barrier and overtopping deposit, mass transport deposits, argillaceous sediment.
(5) The analysis of the granularity of LS33-1-1and LS22-1-1well shows that, the average grain size of sediments is generally decreasing from yacheng formation to yingghai formation. Depositional environment of qiongdongnan basin changed from lake facies, near-shore facies, epeiric sea facies, to shallow sea-bathyal deposits, and it reflects that hydrodynamic condition is generally decreasing.
琼东南盆地位于南海北部大陆边缘,是新生代形成的断陷盆地。其构造演化上的特征为“下断上坳”,以破裂不整合面T60为界,经历了古近纪裂陷阶段和新近纪的裂后热沉降阶段。根据断裂发育情况以及盆地充填变形特征,将裂陷和裂后两大演化阶段进一步细分为4个构造幕,分别是裂陷Ⅰ幕(始新世-早渐新世断陷期)、裂陷Ⅱ幕(晚渐新世断坳期)、裂后Ⅰ幕(早-中中新世热沉降期)和裂后Ⅱ幕(晚中新世-第四纪加速沉降期)。
本文以国家科技重大专项—“南海北部深水区潜在富生烃凹陷评价”中的子课题“南海北部深水区古气候和古环境研究”(2011ZX05025-002-03)为依托,以琼东南盆地深水区油气钻井LS33-1-1井和LS22-1-1井及贯穿琼东南盆地的十几条地震剖面为研究对象,通过地震与古生物地层标定,结合测井与沉积物粒度分析,建立了琼东南盆地等时层序地层格架,探讨了琼东南盆地沉积相和深水区沉积充填特征,为今后琼东南盆地石油勘探奠定了基础。论文主要成果包括：
(1)通过地震地层和古生物地层标定,建立了LS22-1-1井和LS33-1-1井两口深水探井的年代地层框架。主要的地层单元包括：始新统岭头组,渐新统崖城组和陵水组,中新统三亚组、梅山组和黄流组,上新统莺歌海组,地层的地震界面分别为T100(始新统底界)、T80(32Ma)、T70(28.4Ma)、T60(23Ma)、T50(16.OMa)、T40(11.6Ma)、T30(5.5Ma)和T20(1.8Ma)。在32～1.8Ma的地层中,共识别出一级层序界面1个(T60),二级层序界面6个(分别是T100、T80、T70、T60、T40、T20)。以T60为界将地层分割为两个一级层序。以T100(始新统底)、T80(始新统顶)、T70(崖城组顶)、T60(陵水组顶)、T40(梅山组顶)、T20(莺歌海组顶)为界,将地层分割为5个二级层序。建立了包含18个三级层序的琼东南盆地的层序地层格架。划分出T60-T20各三级层序内的低位体系域、海进体系域和高位体系域共28个
(2)通过LS33-1-1和LS22-1-1两口深水探井古生物资料,利用生物化石(主要为浮游有孔虫和钙质超微化石)基准面的年龄值,确定钻孔中年龄与深度的对应关系,建立了生物年代序列和等时层序地层格架,为油气地质条件分析和古环境恢复奠定了基础。
(3)根据陆坡体系的外部形态及其内部沉积构成特征,在空间上自西向东可以将其划分为为4类：进积型陆坡、滑塌型陆坡、水道化型陆坡和宽缓单斜型陆坡。在陆坡上发育了：陆坡峡谷、浊流沉积、滑塌沉积、碎屑流沉积、滑移沉积和沉积物波等沉积类型。
(4)琼东南盆地中央峡谷呈北东向展布,平面形态呈“S”型；西段起源于莺歌海盆地中部,向东经乐东、陵水、松涛、宝岛、长昌5大凹陷,最后延伸进入西沙海槽。在中央峡谷充填了块体流、天然堤及漫溢沉积、深海泥质沉积、浊积水道、浊积席状砂等沉积微相。峡谷西段的乐东凹陷和陵水凹陷的西部以浊积水道沉积为主,东段为浊积水道与块体流沉积互层沉积,浊积水道和浊积席状砂是深水区油气勘探的主要储层类型。
(5)通过对琼东南盆地LS22-1-1井、LS33-1-1井岭头组、崖城组、陵水组、三亚组、梅山组和黄流组和莺歌海组地层的粒度资料分析,结果表明从始新世岭头组到上新世莺歌海组,沉积物的平均粒径总体上呈减小的趋势。盆地的沉积环境经历了湖相、滨岸相、陆表海相向浅海-半深海环境的演变,水动力条件从强到弱。
The South China Sea is a huge marginal sea at the western Pacific.The boundary of north is China continental margin;The boundary of west is near the Yinzhi continent;The boundary of south is near Kalimantan island;The boundary of east is near Marnila trench.The South China Sea is located in convergence parts of the Pacific plate、Indian-Australian plate and Eurasian plate.For the reason of subducting the Pacific plate to Eurasian plate,collision orogeny Indian-Australian plate to Eurasian plat, covergence Palawan and ReedBank to Kalimantan island. These tectonic activity cause the present tectonic framework of the South China Sea:the north is passive continental margin,the east is subduction belt, the south is covergence belt, the west is strike-slip shearing belt.The South China Sea stopped expanding from the end of the early Miocene(16.7Ma). During the expansion process, The South China Sea developed a wide range of depositional basin, which received a large amount of land-sourced material,riching in organic matter, and had good hydrocarbon source rock, transporting and storage of petroleum geological conditions. The deep water hydrocarbon prospective areas in the Northern South China Sea become the consensus of the international community.
The Qingdongnan basin is located in the Northern South China Sea, which is a graben basin during Cenozoic. Its bottom half is graben basin, the top half is sag basin. The boundary between two half is seismic interface T60. Throughout the period of geological history, the South China Sea has main undergone rift epoch from Paleocene to early Oligocene, Rift fault-depression-squeeze reversed in late Oligocene and the sedimentation period from the early Pliocene to Quaternary.
This paper is based on major national technology special project "The research on The evaluation about the potential rich hydrocarbon Sag in deepwater area of Northern South China Sea"-branch project:"The research of paleoenvironment and paleoclimate in deepwater area of Northern South China Sea"(2011ZX05025-002-03), basing on the paleontology information of the oil and gas well LS22-1-1、LS33-1-1and more than ten seismic profile. Analysing of the LS22-1-1、LS33-1-1well about the seismic interface icons of palaeontogical fossils data, log information, grain size of sediment, and then giving isochron sequence stratigraphic framework, analysis the sedimentary facies and depositional characteristics of deepwater area in Qingdongnan basin, give help to oilexploration in the future. The main conclusions are as follows:
(1) Analysing of the LS33-1-1and LS22-1-1well about the seismic interface icons of palaeontological fossils data, and then giving paleontological stratigraphic division for the two wells. The main stratigraphic formation includes:eocene-lingtou formation; oligocene-yacheng and lingshui formation; miocene-sanya、meishan and huangliu formation; pliocene-yinggehai formation. The seismic interfaces are respectively T100、T80(32Ma)、T70(28.4)、T60(23.0Ma)、T50(16.0Ma) T40(11.6Ma)、T30(5.5Ma)、T20(1.8Ma). During32-1.8Ma, we recognise1primary sequence interface(T60),6sencondary sequence interface(T100、T80、T70、T60、 T50、T40、T30、T20), including2primary sequences、5sencondary sequences and18tertiary sequence stratigraphy, we recognise28low stand tract, transgressive stand tract and high stand tract.
(2) Quantitative bio stratigraphic analysis methods were used to study the paleontological data of the LS33-1-1and LS22-1-1well, we determine the sequence interface age and the corresponding relation of age and depth,establish the biological sequence and isochronal sequence stratigraphic framework.
(3) According to the slope system external form and its internal deposit formation, which can be divided into4classes from the west to the east:progradation slope, slumping slope, Channel change slope and Rolling monoclinic slope. Sedimentation type includes:Slope canyon、turbid flow、slumping、debris flow、slide and sediment waves.
(4) The central valley is "s" type in the plane, extended direction NE. Originating from yinggehai basin to xisha trough,the central valley goes through ledong sag,lingshui sag, songtao sag, baodao sag and changchang sag.The sedimentary facies in The central valley includes5types,such as:turbidity channel, turbidite sand sheet,natural barrier and overtopping deposit, mass transport deposits, argillaceous sediment.
(5) The analysis of the granularity of LS33-1-1and LS22-1-1well shows that, the average grain size of sediments is generally decreasing from yacheng formation to yingghai formation. Depositional environment of qiongdongnan basin changed from lake facies, near-shore facies, epeiric sea facies, to shallow sea-bathyal deposits, and it reflects that hydrodynamic condition is generally decreasing.
引文
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