Distribution of Pre-Cenozoic strata and petroleum prospecting directions in China Seas
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摘要: 经过60年的油气调查与勘探，随着中国近海新生代盆地的勘探程度不断提高，油气发现难度逐渐加大，海洋油气勘探新领域的开拓成为当务之急。近年来的调查与勘探发现，中国海域前新生代盆地残留地层具有如下特征：① 厚度大，一般为4000～6000 m，最大厚度超过9000 m；② 分布广，有渤海、北黄海、南黄海、东海-南海北部和南海南部5大分布区；③ 存在新元古界、下古生界、上古生界、中生界“下部层系”、中生界“中部层系”和中生界“上部层系”6套地层；④ 可划分东海-南海型和渤海-黄海型两类层型结构，前者仅由“单一”的中生代地层组成，后者由新元古界-古生界-中生界“叠合”构成；⑤ 发育下寒武统、下志留统、石炭系、二叠系、侏罗系和白垩系6套烃源岩，其中下寒武统、下志留统和二叠系烃源岩有机质丰度高，侏罗系烃源岩分布最广；⑥ 具有孔隙型、裂缝改造型和风化壳型3类储层，其中，孔隙型储层包括白云岩、礁滩相碳酸盐岩和砂岩储层，裂缝型储层与大型断裂带和挤压构造带伴生，风化壳储层可分前寒武系变质岩和混合花岗岩、古生代碳酸盐岩、中生代火山岩以及花岗岩、中生代碎屑岩4亚类，其物性及分布主要受构造作用、风化淋滤作用和埋藏条件3种因素控制；⑦ 具备“古生古储”、“古生中储”、“古生新储”、“中生中储”、“中生新储”和“上生下储”6类成藏组合。综合分析认为：中国海域前新生界油气前景广阔，南黄海海相中-古生界、东海南部-南海北部海域中生界、新生代富生烃凹陷内的潜山是中国海洋油气下一步勘查方向；北黄海盆地坳陷区的中生界和渤海海域的前新生界“自生自储”油气藏值得重视。Abstract: After 60 years of oil and gas investigation and exploration, the exploration degree of Cenozoic basins and the difficulty of oil and gas discovery in offshore China has increased, and the development of new fields for offshore oil and gas exploration has become an urgent task. Surveys and explorations in recent years have found that characteristics of the residual strata in the Pre-Cenozoic basins in offshore China could be summarized as follows: ① Huge thickness. The thickness of the Pre-Cenozoic varies in the range of 4000～6000 m with a maximum over 9000 m; ② Wide distribution. Pre-Cenozoic Strata are found in five major areas, i.e. the Bohai Sea, the North Yellow Sea, the South Yellow Sea, the East China Sea–the northern South China Sea and the southern South China Sea from north to south; ③ Six sets of strata, which include the Neoproterozoic, the Lower Paleozoic, the Upper Paleozoic, the Lower Mesozoic, the Middle Mesozoic, and the Upper Mesozoic; ④ Two types of stratigraphic architectures, i.e. the type of East China Sea-South China Sea composed only by the Mesozoic, and the type of Bohai-Yellow Sea superimposed by the Neoproterozoic, Paleozoic, and Mesozoic; ⑤ Six sets of source rocks, which include the Lower Cambrian, the Lower Silurian, the Carboniferous, the Permian, the Jurassic, and the Cretaceous source rocks, among which the Lower Cambrian, the Lower Silurian, and the Permian source rocks have the highest organic matter content, and the Jurassic source rocks distribute the most widely; ⑥ Three kinds of reservoirs, namely the porous reservoirs, the fracture-modified reservoirs, and the weathering crust reservoirs. The porous reservoirs mainly consist of dolomite, reef-bank carbonate, and sandstone, and the fracture-modified reservoirs are often associated with large fault zones and/or compressive structural zones, and the weathering crust reservoirs can be further divided into four sub-types: Precambrian metamorphic rocks and magmatic granite, Paleozoic carbonate rocks, Mesozoic volcanic rocks and granite, and Mesozoic clastic rocks. The physical properties and distribution of reservoirs are mainly controlled by tectonics, weathering and leaching process, and burial conditions; ⑦ Six types of plays from the Paleozoic source to the Paleozoic reservoir, from the Paleozoic source to the Mesozoic reservoir, from the Paleozoic source to the Cenozoic reservoir, from the Mesozoic source to the Mesozoic reservoir, from the Mesozoic source to the Cenozoic reservoir, and from the Cenozoic source to the Pre-Cenozoic reservoirs. In conclusion, the Pre-Cenozoic petroleum has great potential and broad prospects in China Seas. Next exploration targets should be focused on the marine Mesozoic-Paleozoic in the South Yellow Sea, the Mesozoic-Cenozoic in the southern East China Sea and the northern South China Sea, and the buried hills in Cenozoic hydrocarbon-rich depressions. The Mesozoic in the North Yellow Sea and the self-generating source to self-storing reservoirs in the Pre-Cenozoic of the Bohai Sea should be paid attention.
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Keywords:
- China Seas /
- Pre-Cenozoic /
- stratigraphic distribution /
- petroleum prospecting
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碳酸盐岩油气田是全球油气最重要的组成部分，其常规油气储量约占全球油气总储量的60%，产量约占50%[1]。中国海相碳酸盐岩经历了40多年的油气勘探，随着上扬子四川盆地威远、普光、龙岗和元坝等多个大型碳酸盐岩油气田的发现，证明碳酸盐岩是扬子区油气开采的重要领域之一[2-4]。南黄海盆地是下扬子板块向东延伸的主体，为前震旦纪变质岩基底之上的一个多旋回叠合盆地，与四川盆地具有相似的地质结构和演化历史，但同时又具有其自身的特点[5-8]，其油气勘探一直是海洋石油地质学家和地球物理学家关注的焦点[9-12]。南黄海盆地经过多年的油气勘探，始终没有获得油气的重要发现，为目前我国近海海域唯一一个尚未获得油气突破的大型沉积盆地[13-16]。
海域已有钻井证实南黄海崂山隆起中—古生代地层发育多套海相碳酸盐岩，但由于印支、燕山构造运动对中—古生界原型沉积的改造，中—古生代地层构造特征复杂，加上碳酸盐岩储层非均质性强，因此，碳酸盐岩储层预测是南黄海油气勘探的重点和难点[17-18]。
碳酸盐岩储层包括孔隙型、裂缝型和孔隙-裂缝复合型，孔隙型碳酸盐岩储层包括礁滩相和白云岩型，礁滩相储层主要以川东北普光和元坝油气田的长兴组-飞仙关组礁滩[19]以及南海的古、新近纪生物礁为例[20]；白云岩储层以川中下寒武统龙王庙组为例[21-22]。对于礁滩相碳酸盐岩储层预测，许多学者通过对碳酸盐岩进行岩石物理分析，认为其基质具有非均质性且孔隙结构多变的特点，同时提出不同的岩石物理模型进行流体替换，从而获得碳酸盐岩在不同条件下的纵横波速度和各向异性特征[23-27]，此外通过AVO正演模拟发现碳酸盐岩储层中的孔隙性和含油气性差异可以引起明显的AVO异常[28-30]。随着近几年地球物理技术的发展，碳酸盐岩储层预测技术从地震属性分析[31-33]发展到叠后波阻抗反演[34-36]、叠前统计学反演[37-40]、叠前同时反演方法[41]以及相控约束下的地震反演方法等[42-44]，这些方法在碳酸盐岩储层预测中均得到了较好的应用。另外，时频分析方法也逐渐应用于碳酸盐岩的含油气预测研究[45-47]，尤其是对复合型储层的含油气性预测得到了很好的验证[48]。
关于南黄海碳酸盐岩储层预测方面研究，前人运用岩石物理分析[49]、地震属性分析[50-51]、叠前反演[52-54]和时频分析[55-56]等方法开展了储层特征相关的研究工作，但鲜有对孔隙型碳酸盐岩储层做系统分析和预测，且目的层没有聚焦。本文利用钻遇石炭系—下二叠统的测井资料和研究区的地震资料，通过分析南黄海石炭系—下二叠统孔隙型碳酸盐岩储层特征，结合岩心资料的岩石物理分析，提取孔隙型碳酸盐岩的岩性和物性敏感弹性参数，运用叠前同时反演方法对崂山隆起孔隙型碳酸盐岩储层进行预测，预测了有利储层的分布特征，并对其进行了分析。
1. 沉积背景
南黄海盆地面积18万km2，现今盆地的构造格局南以勿南沙隆起、北以千里岩隆起为界，盆地从南到北可以划分为青岛坳陷、崂山隆起和烟台坳陷3个二级构造单元（图1）[13, 52]。盆地进行了7.8×104 km的二维地震测量，4口井钻遇石炭系—下二叠统，如CZ35-2-1井、CZ12-1-1井、WX13-3-1井和CSDP-2井[11, 57-58]，其中CSDP-2井在石炭系—下二叠统碳酸盐岩见油气显示，岩心样品中也发现了大量的油气包裹体，说明南黄海石炭系—下二叠统碳酸盐岩地层具备一定的油气潜力[11, 59-61]。
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早石炭世的全球海侵使下扬子板块与华夏板块形成了巨大的碳酸盐岩台地，直至船山组末期海退结束。石炭纪—二叠纪时期，下扬子板块位于北半球低纬度地区，为热带温暖湿润气候，大气降水充沛，有利于碳酸盐岩沉积[62-64]（图2a）。早石炭世初期（金陵组和高骊山组），地层沉积较薄，主要为碎屑岩[65]（图2b）；早石炭世晚期盆地开始沉降，海水从盆地东、西两面入侵，和州组期间南黄海盆地由东向西沉积，呈NNE向浅水陆棚相和潮坪-潟湖相，岩性以灰岩和白云质灰岩为主；晚石炭世初期海侵规模最大，扬子海与华南海几乎连成一片，普遍为浅海相碳酸盐岩沉积环境，岩性为致密纯灰岩，南黄海盆地从东向西沉积了NE向开阔台地相、局限台地相及潮坪相。黄龙末期整体抬升，露出水面，部分地层遭受剥蚀，黄龙组与上覆船山组呈假整合接触。晚石炭世船山组初期，海水再次入侵，沉积整体向SE迁移，南黄海盆地从东向西沉积了呈近似NE向的开阔台地相、局限台地相及潮坪相，在局部高地发育了生物礁滩相。早二叠世栖霞期为晚古生代以来最大的一次海侵期，普遍沉积了富含䗴类、珊瑚、有孔虫和钙藻为主的生物碎屑灰岩，形成了稳定岩相和厚度的南方巨型碳酸盐岩[66]，早二叠世晚期，下扬子区开始海退，全区大部分转变为海陆交替的三角洲和潟湖海湾沉积，结束了海相沉积历史。
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图 2 沉积相、岩性和地震解释剖面综合分析a. 南黄海晚石炭世船山期沉积相，红色框为本文研究区；b. 石炭世—二叠世岩性简化柱状图；c. 地震解释剖面（黑色箭头分别表示剖面的位置和石炭系—下二叠统对应的岩性）。Figure 2. Integrated profiles of sedimentary facies，lithology and seismic interpretationa. The sedimentary facies map of the Late Carboniferous Chuanshan period in the South Yellow Sea, the red border is the research area of this paper;b. Simplified lithologic column charts from Carboniferous to Permian; c. seismic interpretation profile （Black arrows indicate the location of the profile and the corresponding lithology of the Carboniferous- Lower Permian）.石炭系—下二叠统在地震反射剖面上为T10- T11之间的一套反射层，T10为顶面，表现为一套中—低频强波峰的反射，T11为底面，表现为中— 低频强波谷的反射，T10与T11反射界面呈平行反射特征（图2c），顶底之间时间差为200～260 ms，地层厚度为550～715 m，内部整体为较连续、中频、中振幅、平行—亚平行的反射结构，局部存在丘状反射，说明地层厚度整体比较稳定、分布广泛，由于受到后期印支运动的影响，局部高部位被剥蚀。
2. 碳酸盐岩储层特征
2.1 岩石物性特征
南黄海孔隙型碳酸盐岩储层形成于高能沉积环境，常见核形石、鲕粒或生物碎屑灰岩[67]。崂山隆起CSDP-2井揭示上石炭统船山组1724.7～1757.78 m和1762～1792.4 m发育大量的灰色—深灰色生物碎屑灰岩，根据岩心观察，储层为晶间孔、粒内孔和生物碎屑溶蚀孔，解释为台内滩相[3, 68-69]，藻灰岩孔隙度为0.56%～12%，平均5.61%，渗透率小于0.01 mD（图3）。位于青岛坳陷的CZ12-1-1井在石炭系同样发育生物碎屑灰岩储层，厚133 m，船山组中—下部由褐灰色藻团细粉晶灰岩、深灰色含生物粉晶灰岩组成，上部为浅灰色生物藻团粉晶灰岩、灰色生物细碎屑粉晶灰岩、泥晶灰岩和含燧石灰岩，生物碎屑灰岩孔隙度为8%～14%，平均为10.6%，渗透率为1～4.2 mD，平均为2.13 mD。对比四川盆地的碳酸盐岩岩石物性[70-71]，南黄海盆地石炭系碳酸盐岩储层的孔、渗物性条件较好。
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图 3 CSDP-2井上石炭统船山组生物碎屑灰岩柱状图和岩心照片a. 船山组岩心柱状图，箭头表示岩样分析位置；b. 1 730.4 m生物碎屑泥晶灰岩；c. 1 757.03 m生物碎屑亮晶灰岩充填孔；d. 1 777.83 m生屑泥晶灰岩；e. 1 819.5 m灰岩晶间孔。Figure 3. The lithologic column and core photographs of upper Carboniferous Chuanshan Formation of Well CSDP-2a. Lithologic Column of the Chuanshan Formation, arrows indicate the location of the samples analyzed; b. Bioclastic micritic limestone at depth of 1 730.4 m; c. Bioclastic sparry limestone filled pore in the depth of 1 757.03 m; d. Bioclastic micrite limestone in the depth of 1 777.83 m;e. Limestone intergranular pore in the depth of 1 819.5 m.2.2 测井-地震响应特征
以青岛坳陷的CZ12-1-1井为例，分析以生物碎屑灰岩为典型代表的井- 震响应特征，该井在上石炭统船山组中揭示了137 m厚的生物碎屑灰岩，其速度为5 000～6 000 m/s，密度为2.3～2.6 g/cm3，纵波阻抗为16 000～17 000 g/cm3·m/s，位于船山组上部的始新统碎屑岩地层速度为2 300～3 000 m/s，密度为2.2～2.3 g/cm3，阻抗为5 500～6 200 g/cm3·m/s，由于受逆断层的影响，下部夹杂二叠系梁山组薄层碎屑岩，其速度为3 000～4 000 m/s，密度为2.2～2.4 g/cm3，阻抗为7 000～8 000 g/cm3·m/s，可见船山组生物碎屑灰岩相对碎屑岩地层为高速高阻抗的曲线特征，与下部的黄龙组等灰岩地层的阻抗差异较小。在地震剖面上，船山组顶部的生物碎屑灰岩为强振幅连续反射，内部为断续—较连续的强反射特征，船山组与上部始新统和下部的梁山组碎屑岩之间形成2个波峰和1个波谷的强反射，其下部和州组和黄龙组的灰岩内幕为较连续— 断续反射特征（图4）。
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图 4 CZ12-1-1井测井曲线和地震响应特征Figure 4. Logging and seismic characteristic of Well CZ12-1-12.3 敏感参数分析
利用CSDP-2井岩心实测的纵波阻抗与横波阻抗进行交汇分析（图5），纵波阻抗可以较好地区分岩性变化，能够统计出砂岩和灰岩的纵波阻抗分布范围，其中砂泥岩的纵波阻抗为10000～14500 g/cm3·m/s；纯灰岩纵波阻抗为13800～16300 g/cm3·m/s，生物碎屑灰岩的纵波阻抗为16300～17500 g/cm3·m/s，表明纵波阻抗能够区分碎屑岩、纯灰岩和生物碎屑灰岩，因此纵波阻抗成为岩性区分的敏感弹性参数。
为获取储层的物性敏感弹性参数，将CSDP-2井实测的灰岩（包括纯灰岩和生物碎屑灰岩）孔隙度划分成不同等分，将纵波速度、横纵波速度及密度数据由岩石物理方程计算得到弹性参数，对弹性参数进行两两交汇分析，筛选对物性敏感的弹性参数，为下一步储层预测提供参考依据。由交汇分析可知，随着孔隙度的增加，拉梅常数λ和泊松比（图6a）、纵波阻抗和体积模量K（图6b）、剪切模量μ和纵波速度Vp（图6c）数值均呈减小趋势，单纯依靠这些弹性参数区分物性会有重叠，由图6d可以看出，低λρ（拉梅常数和密度乘积）和μρ（剪切模量和密度乘积）的灰岩具有好的物性，且两者的重叠区间相对较小，因此，本文选择λρ来判断储层物性好坏，将目的层段灰岩的λρ与孔隙度进行交会分析（图7），得到两者的线性关系φ=λρ×10−9+1.3052。
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图 7 CSDP-2井石炭系—下二叠统生物碎屑灰岩段的λρ与孔隙度拟合Figure 7. Fitting relationship between λρ and porosity of bioclastic limestone from Carboniferous to Lower Permian of Well CSDP-23. 孔隙型碳酸盐岩预测技术
南黄海石炭系—下二叠统沉积相在横向上分布存在变化，因此其对应的岩性也存在变化，同时由于成岩作用和构造作用，碳酸盐岩储层的物性也会有所不同，需要根据研究区碳酸盐岩岩石物理特征，选择合适的地震反演方法，系统分析有利储层的分布范围。一般情况下，影响地震反演结果的因素主要为地质条件和针对性方法的选择，其中方法选择的关键因素主要有地震资料的品质、井震标定的子波提取、低频模型建立和反演过程参数的选取。因此采用合适的针对性技术手段和思路非常重要[72-73]。本文根据南黄海井点的岩石物理分析得到储层的岩性和物性敏感弹性参数，采用叠前同时反演方法进行石炭系—下二叠统的碳酸盐岩储层预测。具体反演过程为：首先根据不同角度道集的井震标定合成地震记录，获得井旁道远、中、近道集的地震子波；其次结合井点空间插值速度模型和高精度层析速度反演结果，建立低频速度模型；最后通过对优化后的CRP道集，采用叠前同时反演方法，对南黄海石炭系—下二叠统碳酸盐岩的岩性和物性进行预测，最终获得研究区孔隙型碳酸盐岩的有利储层分布特征，具体技术流程如图8。
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图 8 南黄海叠前同时反演储层预测技术流程Figure 8. Flow chart of pre-stack simultaneous inversion for reservoir prediction3.1 子波提取
基于CSDP-2井测井曲线进行精细的合成地震记录分析，首先利用雷克子波进行初步的井震标定，然后根据实际井旁地震道提取最小相位子波及零相位子波分别制作合成记录，地震资料频谱为8～50 Hz，主频为25 Hz，通过合成地震记录，得到了全叠加子波，经过大量的合成记录对比分析，发现从该井井旁地震道提取的非零相位子波效果最佳。由图9a可以看出，CSDP-2井合成地震记录与实际地震道的匹配一致，说明提取的子波非常准确，进而确定了该井的时深关系。在此基础上，选取3个不同角度道集的部分叠加地震道集，通过远、中、近道集合成地震记录提取3个不同角度的子波，用于下一步叠前同时反演（图9b）。
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图 9 CSDP-2井合成地震记录及提取子波（a. 全叠加数据合成地震记录，b. 远、中、近叠加道集合成地震记录， c. 不同叠加道集提取的近、中、远角度子波，d. 不同角度提取子波的能量谱 ）Figure 9. The synthetic seismogram and extract wavelets of the Well CSDP-2（a. synthetic seismogram from full stack seismic, b. synthetic seismogram from far-mid-near stack seismic, c. wavelets extracted from far-mid-near synthetic seismogram, d. energy spectrum of wavelets extracted from different angles）3.2 低频模型建立
海洋地震资料频谱普遍缺失8 Hz以下的数据信息，因此进行叠前同时反演时，需要根据纵波阻抗、横波阻抗和密度模型，来补全低频信息。首先对速度测井曲线空间插值，即通过精细的地层解释来建立地层格架，再进行井间曲线内插；其次将叠加速度谱的层析反演结果作为低频速度模型，将低频速度模型与井间插值结果两部分的模型进行叠加，从而得到低频纵波速度模型；最后对井点速度、纵横波阻抗以及密度统计结果进行拟合转换，最终得到纵波阻抗、横波阻抗和密度低频模型。
3.3 叠前同时反演储层预测
地震阻抗反演的最终目的是半定量- 定量地预测碳酸盐岩的储层分布以及物性特征，本文通过分角度叠加地震道集资料，在纵波阻抗、横波阻抗和密度低频模型的约束下进行叠前同时反演，从而得到纵波阻抗的岩性数据和λρ的物性数据（图10a和10b），根据岩石物理分析的结果，区分碎屑岩和灰岩的纵波阻抗门槛值为13500 g/cm3·m/s，区分生物碎屑灰岩和纯灰岩的纵波阻抗门槛值为16300 g/cm3·m/s，图10a中纵波阻抗值红色部分代表生物碎屑灰岩，黄色代表纯灰岩，蓝色代表碎屑岩。可以看出石炭系—下二叠统栖霞组生物碎屑灰岩储层比较发育，主要在石炭系和州组和船山组，以及下二叠统栖霞组局部分布。结合图10b中λρ显示的物性剖面（3～6）×107（kg2/m2·s）为灰岩段有利物性储层，图中红黄色表示物性最优，绿、蓝色表示物性较好。根据波阻抗门槛值去掉碎屑岩和纯灰岩的阻抗范围，结合岩石物理分析结果，得到λρ与孔隙度的拟合关系（图7），最终得到孔隙型碳酸盐岩储层的孔隙度数据体（图10d），可以看出石炭系孔隙型碳酸盐岩储层表现出较强的非均质性，且横向分布具有一定的不连续性，位于北东方向古高地处物性较好，孔隙度较高，为7.5%～12.5%。
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图 10 叠前同时反演结果a. 纵波阻抗剖面代表岩性分布，b. λρ剖面代表物性优劣，c. 下石炭船山组物性切片，d. 孔隙度剖面。Figure 10. Pre-stack simultaneous inversion resultsa. Longitudinal impedance profile-representing lithologic distribution; b. λρ profile-representing physical properties; c. Physical properties section of lower Carboniferous Chuanshan Formation; d. porosity profile.4. 孔隙型碳酸盐岩成因分析
扬子板块石炭系—下二叠统的古纬度为1.6°S，位于赤道附近的热带海洋环境地带，温暖海水有利于碳酸盐岩发育[62]。这段时期南黄海盆地的水体较四川盆地深，因此孔隙型碳酸盐岩不像四川盆地大范围分布，仅发育于四周被广海陆棚或槽棚相所围限的碳酸盐岩台隆边缘。南黄海崂山隆起为加里东期之后的继承性古隆起[74]，局部高地主要发育礁滩相台地，且礁滩体展布多受局部构造所控制，其形成常与古隆起和古断裂作用有关。此外台地边缘的张性断裂在地层缓慢的沉积过程中为生物礁的生长提供了可容空间和深部的营养成分。
研究区碳酸盐岩沉积过程中存在较高的孔隙度，但由于地层的埋藏压实作用，原生孔隙均相继被充填，后期受印支运动作用，上覆地层被抬升到地表遭受暴露，在古高地附近的石炭系—下二叠统孔隙型碳酸盐岩发生大气淡水淋滤和溶蚀作用，使得次生孔隙发育，以溶孔、粒间、粒内孔为主的复杂组合为主。南黄海崂山隆起已有钻井CSDP-2井在石炭系船山组和黄龙组钻遇生物碎屑灰岩，且在该段地层岩心中多处见到油气显示，较好证明了石炭系—下二叠统的生物碎屑灰岩为有利储层段，因此寻找高孔隙性的孔隙型碳酸盐岩是研究区优选目标。
5. 结论
（1）根据井点岩石物理分析，声波阻抗为岩石敏感弹性参数，不仅能够区分碎屑岩和碳酸盐岩，而且能够区分生物碎屑灰岩和纯灰岩；λρ为物性敏感弹性参数，其具有随着孔隙度增高而减小的特点。
（2）采用叠前同时反演方法对孔隙型碳酸盐岩储层预测，结果表明南黄海崂山隆起石炭系—下二叠统生物碎屑灰岩比较发育，纵向上主要发育在石炭系和州组和船山组，以及下二叠统栖霞组局部发育，横向上位于研究区北东方向古高地处物性较好，为7.5%～12.5%高孔隙度。
（3）结合已有钻井碳酸盐岩岩心和盆地构造特征，分析认为受印支期构造运动影响，石炭系—下二叠统碳酸盐岩遭受淡水淋滤和溶蚀作用，次生孔隙比较发育，以溶孔、粒间、粒内的组合孔隙为主。
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图 3 东海-南海型前新生代地层层序
Figure 3. Pre-Cenozoic stratigraphic sequence of the East Sea-South Sea type
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图 4 渤海海域石炭系—二叠系残留厚度
Figure 4. Residual thickness of the Carboniferous system -Permian system in the Bohai Sea area
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图 5 南黄海海域震旦系—下三叠统残留厚度
Figure 5. Residual thickness of the Sinian system – the Lower Triassic system in the South Yellow Sea Area
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表 1 中国海域前新生代地层及最大厚度
Table 1 Distribution of Pre-Cenozoic strata in China Seas (strata type and maxmum thickness）
m 地层层序 渤海 黄海 东海-南海北部 南海南部 北黄海 南黄海 东海 台湾海峡 台西南 南海北部 巴拉望 礼乐 中生界 上部层系 3000 4000* 3000 3500* ＞1082 3000* 3500* 3000* 4000* 中部层系 1000 2000 ＞2195 4500* 缺失 600 5300* 缺失 缺失 下部层系 1200 1500 3000* ？ ？ ？ ？ ？ ？ 古生界 上古生界 1400 ＞2000 4500* ？ 缺失 缺失 缺失 ？ ？ 下古生界 ＞310 ＞472 4500* ？ 缺失 缺失 缺失 缺失 缺失 元古界 新元古界 不详 ＞931 1200* 缺失 缺失 缺失 缺失 缺失 缺失 叠合面积 67616 km2 43279 km2 183917 km2 419433 km2 608921 km2 层型结构 “叠合型”（新元古界-古生界-中生界） “单一型”（中生界） 注：表中*为地震资料解释最大厚度；？表示情况不明。 
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表 2 下扬子区下寒武统幕府山组烃源岩厚度及有机质丰度
Table 2 Statistical table of thickness and total organic abundance of source rocks in the Lower Cambrian Mufushan Formation in the lower Yangtze region
序号 井号 厚度/m TOC/% 最小 最大 平均 1 苏东121井 368 0.55 4.84 3 2 皖2井 465 0.57 10 3.6 3 官地1井 442 0.51 47.7 9.82
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表 3 中国海域潜山油气藏生储盖组合特征
Table 3 Characteristics of source rock, reservoir and cap rocks assemblages of buried hill reservoirs in China Seas
潜山油气藏 构造 地层时代 烃源岩（层位） 储层岩性 盖层（层位） 蓬莱9-1 庙西北凸起 中生界 沙河街组及东营组 二长花岗岩 馆陶组 锦州25-1S 辽西北凸起 太古界 沙河街组及东营组 二长片麻岩、斜长片麻岩 沙河街组及东营组 曹妃甸11-6 沙垒田凸起 太古界 东营组 混合化黑云母花岗岩 馆陶组 曹妃甸18-2 沙垒田凸起 太古界 东营组 二长花岗岩 馆陶组 渤中26-2 渤海凸起 太古界 沙河街组及东营组 英云闪长岩、花岗闪长岩 东营组及明化镇组 锦州20-2 辽西低凸起 太古界 沙河街组及东营组 混合岩、碎屑岩 沙河街组及东营组 渤中19-6 渤中凹陷 太古界 沙河街组 变质岩 沙河街组与东营组 渤中13-2 渤中凹陷 太古界 沙河街组及东营组 花岗片麻岩 中生界 渤中28-1 渤南凸起 古生界奥陶系 沙河街组 碳酸盐岩 沙河街组 岐口17-9 岐口凹陷 中生界 海沟房组、沙河街组 碎屑岩 沙河街组 428W、428E 石臼坨凸起 古生界 沙河街组及东营组 花岗岩 东营组 曹妃甸2-1 沙垒田凸起 古生界 沙河街组 碳酸盐岩 沙河街组 涠6-1、涠10-3N等 涠西南凹陷 古生界 流沙港组 碳酸盐岩 流沙港组 惠州26-6 惠州凹陷 中生界 文昌组、恩平组 花岗岩 文昌组、珠海组 永乐8-1 松南低凸起 中生界 始新统、渐新统崖城组 花岗岩 中新统
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