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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河口水下三角洲是由河流携带的沉积物堆积形成的水下地质体，是流域物质沉积和侵蚀的重要载体，它记录了流域环境的演变历史，包括自然变化过程和人类活动的影响痕迹[1]，因此对其研究具有重要意义。水下三角洲的发育受到入海水沙和海洋动力作用的双重制约，前者使岸线向海延伸、三角洲处于建设阶段，后者使岸线向陆蚀退、三角洲处于衰减阶段[2]。黄河是著名的高含沙河流，中下游以善淤、善决、善徙为特点，自1855年改道入渤海以来，在莱州湾与渤海湾交界处形成沉积厚度约15 m的现代黄河水下三角洲，它是含沙量高的单向淡水流与潮汐、波浪、环流多向咸水流相互作用组成的一个复杂动力系统[3]。
部分学者曾利用实测水深地形资料对黄河废弃水下三角洲进行冲淤演变的研究[4-8]，发现黄河水下三角洲的冲淤演变主要集中在新老河口周围：1968—1976年刁口河口区域形成3个淤积中心且最大淤积厚度都在10 m左右，1976—1996年此区域形成3个侵蚀中心且平均年侵蚀深度在0.4 m左右；研究也表明黄河口改道后，老河口在水深15 m以浅海域冲刷作用最为强烈，水深15 m以深海域冲刷作用较为缓和。可靠的年代数据是研究沉积物环境演变的基础，人工放射性核素137Cs（半衰期30.2a）与自然放射性核素210Pb（半衰期22.7a）作为百年尺度的测年方法被广泛运用于沉积物的定年与沉积速率的计算[9-10]。为了探讨黄河水下三角洲沉积环境的变化以及发育演变的规律，前人利用137Cs与210Pb的研究主要集中在沉积环境和特征方面的变化。李凤业对黄河水下三角洲4个柱状样的210Pb的分析表明，其受到海洋动力及河道变迁的制约出现混合区—衰变区—本底区的多阶段分布，且沉积速率最低为1.29 cm/a，最高为14.52 cm/a[11]。成国栋根据黄河三角洲东部钻孔岩芯的210Pb垂直剖面发现，泥沙的再沉积作用是普遍的，且对210Pb起到了稀释作用[12]。李建芬等研究了渤海湾西岸的210Pb和137Cs的测年情况，发现该地区现代沉积速率从东向西依次为1～3、0.35 和0.1 cm/a, 并划分出了3个相应的现代沉积亚区：开放高潮坪亚区、近端盐沼亚区和远端盐沼亚区[13]。任寒寒对清水沟叶瓣的两个柱状样的沉积物粒度和210Pb活度分布进行分析发现，沉积物粒度组成的突变记录了黄河入海口的变迁以及210Pb活度呈现多阶段和倒置式分布[14]。已有的工作对黄河水下三角洲沉积环境的演变、沉积特征和沉积速率的研究均做出了重要贡献[15-18]，但是在其他因素如黄河入海水沙、海洋动力的变化以及地形演变的综合研究较少涉足。研究表明黄河水下三角洲的137Cs与210Pb活度可能呈现非理想型分布，利用其进行定年与沉积速率的计算也存在诸多不确定性，因此在研究方法与内容上可能稍显单薄。
黄河多次改道，河口海岸地区水动力作用复杂，部分地区沉积环境极不稳定，其中刁口流路水下三角洲作为现代黄河三角洲最后一个废弃叶瓣，发育年代距今不过半个世纪，整个沉积与侵蚀的过程记录也相对完整，为研究三角洲叶瓣演变规律提供了很好的研究素材，具有极高的研究价值。本文通过分析黄河入海口的变迁与入海水沙量的变化探究黄河水下三角洲137Cs和210Pb的分布规律及其影响因素，而后将其与沉积物粒度数据和历史水深数据资料相结合，分别从正演与反演的角度分析刁口叶瓣沉积环境的演变，最后综合考虑黄河口变迁在沉积物粒度和核素活度分布上的表现，并探究三者的对应关系。希望本文的研究成果能够为黄河水下三角洲及类似于本文研究区的河口海岸等地提供核素分布以及沉积特征的理论基础。
1. 样品采集与分析
1.1 样品采集
本文研究区位于黄河三角洲侧缘沉积区，处于最新废弃的黄河口水下三角洲刁口叶瓣东侧（图1）。沉积物柱状样K2（38.2°N、118.9°E）于2014年使用重力取样设备取自黄河口水下三角洲刁口叶瓣，取样处水深约为10 m（2014年实测水深），柱状样长3.5 m，具体采样站位信息如图1所示。柱状样采集后进行密封，并在垂直状态下运输和保存。室内对沉积物柱状样以等10 cm间隔分样后，进行粒度实验与放射性核素活度的分析与测量。
1964年1月，黄河在罗家屋子人工破堤，河水北流入海，这是黄河的第六次改道，1964—1976年，黄河经刁口流路的分流河道进入渤海，而后形成水下三角洲；1976年黄河在西河口（渔洼东北）截流改道，河水东流经清水沟进入渤海，原刁口流路水下三角洲由于缺少泥沙供应，在复杂的海洋动力作用下（波浪、潮汐、潮流等）遭受冲刷和侵蚀，因此本文研究区经历了先淤积后侵蚀的沉积环境的转变。
1.2 实验分析
粒度的分析步骤如下：取适量样品放入洗干净的烧杯中，加入5 mL 30%的 双氧水后摇匀，30 min后加入2 mL约0.1 mol/L的六偏磷酸钠，静置24 h，并用超声波振荡器分散30 min后，用英国Malvern公司生产的Mastersizer 2000型激光粒度分布测量仪进行沉积物粒度测试。仪器测量范围为0.02～2 000 μm，重复测试的相对误差＜2%。
核素的分析步骤如下：将样品置于烘箱中80 ℃烘干，研磨搅拌均匀后制成分装干样。放射性核素210Pb与137Cs采用γ谱仪直接测量的方法，仪器为美国Canberra公司生产的Be-3830的HPGe-γ能谱仪，经表征的BEGe高纯锗平面探测器，探头有效直径70 mm，有效面积3 800 mm2，能量范围10 keV～10 MeV；探测器相对效率＞35%。137Cs的含量用661.62 keVγ射线的全能峰面积计算。210Pb的比活度由46.5 keVγ射线的全能峰面积计算，210Pbex的比活度为210Pb与226Ra比活度的差值，226Ra活度根据351.9keV γ射线的普峰面积计算。137Cs和226Ra的标准样品由中国原子能研究科学院提供。
2. 实验结果
2.1 沉积物粒度变化特征
柱状样K2的沉积物粒度参数如图2所示。沉积物组分以粉砂为主，占总量的60%～82%，均值为73.7%，砂粒含量18%～38.5%，均值为26%；黏粒含量很少且仅有少数层位检出，为1.1%～1.25%。垂向上，沉积物粒度组成以2.1 m为界可明显划分为2段：下段（2.1～3.5 m）沉积物组分以粉砂和砂粒为主，砂粒含量稳定，且不含有黏粒，此阶段平均粒径较小，均值为0.024 mm；上段（0～2.1 m）出现黏粒，砂粒含量明显增大，沉积物组分以粉砂和砂为主，在1.9 m处砂粒含量均达到最大值，为38.5%，此阶段平均粒径较大，均值为0.053 mm。沉积物粒度组分的变化受到沉积环境改变的严重影响，据研究黄河携带泥沙入海后将导致水下三角洲区域沉积物粒度的粗化[19]。
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图 2 柱状样K2的沉积物粒度参数、137Cs活度剖面以及210Pbex活度剖面Figure 2. Sediment grain size composition, activity profile of 137Cs and 210Pbex of K22.2 137Cs活度剖面
柱状样K2的137Cs活度剖面如图2所示。该柱状样137Cs活度范围为（2.6±0.7）～（15.4±1.3）Bq/kg，活度均值为6.2Bq/kg。图中可看出，该沉积物柱状样的137Cs活度剖面存在一个最大蓄积峰和一个次级蓄积峰，最大蓄积峰位于2.7 m处，次级蓄积峰位于1.9 m处（与沉积物粒度组分中砂粒含量最大值出现处相对应），137Cs的放射性活度在1.9 m以深总体水平较高，在1.9 m以浅骤降并始终保持较低水平，两处蓄积峰值活度分别为15.4±1.3Bq/kg和14.4±2.0Bq/kg。
2.3 210Pbex活度剖面
柱状样K2的210Pbex活度分布如图2所示。该柱状样210Pbex活度范围为（5±3.7）～（39±4.6）Bq/kg，整体并未随深度出现指数式衰变，而呈现两段式分布的现象，因此未通过210Pbex获取钻孔处的多年平均沉积速率。图2显示，以1.9m为界，可以将210Pbex活度垂向分布划分为两段：下段（1.9～3.5 m）210Pbex随深度呈指数式衰变，且深度越大越靠近其本底值，为衰变层；上段（0～1.9 m）210Pbex分布异常，违背其衰变规律，出现倒置分布的现象，分析其为混合层，反映此阶段研究区由沉积环境不稳定导致沉积物的快速沉积与侵蚀。本文推测210Pbex的这种阶段分布方式与黄河入海口变迁造成的沉积环境变化具有明显相关性。
3. 讨论
3.1 研究区历史水深变化
本文搜集了黄河水利委员会实测的1：10万研究区历年海图，主要采集到1959、1968、1976、1999、2007、2014年海域内的部分水深数据，底图源于1984、1999、2007与2014年的Landsat遥感影像，后使用ArcGis通过插值——栅格生成6期水深图（图3）。1964年前，黄河未从刁口流路入海，本研究区海底地貌地形基本处于稳定状态，因此将1959年的海底地形视作1964年的初始地形。图3显示，本研究区域地势总体呈现出西南高东北低的趋势，等水深线大体平行于NW-SE方向，与区域内波浪常浪向NE方向相垂直[20]，海底地形的坡度随水深逐渐变缓。
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图 3 研究区1959—2014年各期水深图 （水深依次为1959、1968、1976、1999、2007和2014年；遥感图依次为1984、1984、1984、1999、2007、2014年，黄河口遥感影像始于1984年）Figure 3. Bathymetric map of study area from 1959 to 2014 （water depth for 1959, 1968, 1976, 1999, 2007 and 2014. remote sensing images for 1984, 1984, 1984, 1999, 2007, 2014. Landsat of the Yellow River estuary begins from 1984）比较各期水深图发现，1959—1976年研究区水深快速变浅且等深线快速向海推进；1976—2014年研究区水深逐渐变大且等深线曲折，因此水深变化与黄河入海口变迁相关。1964—1976年（刁口流路行河期），黄河携带大量水沙由刁口入海，研究区快速淤积，海底地貌处于建设期，淤积厚度达5 m；1976年后（黄河改道清水沟），研究区缺乏泥沙供应并在海洋动力（波浪、潮流、潮汐等）的作用下遭受冲刷与侵蚀，近岸河口区域侵蚀作用尤为强烈，海底地貌处于蚀退期，钻孔K2所在区位冲刷厚度达3 m。刘勇等研究发现[21]，黄河口水下三角洲刁口叶瓣1976—1999年的最大冲刷中心与1964—1976年的最大堆积中心吻合，冲蚀厚度达8 m。因此本区域并非侵蚀中心区域，且侵蚀厚度未超过三角洲建设阶段的淤积厚度，于是推断研究区在1964年以前及黄河改道刁口初期的沉积物未遭受侵蚀作用，因此柱状样K2下部（2.1～3.5 m）沉积环境稳定。
3.2 柱状样K2的蓄积峰值
137Cs是20世纪50年代大气核试验产生的放射性核素，据联合国原子辐射科学委员会（UNSCEAR）的报告（2012年）显示，全球137Cs的大气沉降受到地球风带与气压带的影响，因此同纬度圈内137Cs的沉降趋势基本一致，其差异主要由降水量不同导致。本文选取与黄河三角洲位于同一纬度带的东京地区（35°68′98″N、139°69′32″E）参照其137Cs大气沉降趋势（图4）。据日本东京核尘埃沉降监测资料，1963年的137Cs沉降量约占沉降总量的20%，此后137Cs年沉降量骤减并始终保持较低水平；1986年前苏联切尔诺贝利核事故有沉降异常显示，但是远低于核爆期间的年均沉降量，约为1963年沉降量的1/15，且对东亚影响极小[22]。因此在理想的沉积环境下，即区域内未发生混合扰动、侵蚀和再迁移作用，137Cs可测得的起始层位为1954年，最大蓄积峰应出现在1963年，次级蓄积峰应出现在1959年。国内相关研究表明，湖泊与海洋沉积物中的137Cs峰值多对应于1963—1964年，且不应存在1986年的蓄积峰值[23-26]。
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图 4 东京地区1954—2008年的137Cs大气沉降通量Figure 4. 137Cs atmospheric deposition flux from 1954 to 2008 of Tokyo河口及三角洲区域的137Cs除大气沉降输入外，还存在流域侵蚀输入，因此黄河携带大量泥沙入海对研究区的137Cs活度分布产生重要影响。本文根据历年来《中国泥沙公报》和黄河水文站的资料统计黄河于1964—1976年的输沙量（图5）。黄河于1964年1月人工破堤后由刁口流路入海，所携泥沙共计142亿t，这些泥沙在近岸海域快速淤积使得岸线迅速向海推进。历史资料显示，1967年黄河输沙量达最大值，为20.9亿t，1964年次之，为20.3亿t；1967年后，黄河入海泥沙量下降且呈现小幅波动的趋势，这与黄河中上游多个大坝的建立有关。1964年黄河改道刁口流路携带大量泥沙入海，研究区沉积物迅速沉积、核素富集，因此137Cs活度陡然增大，这与137Cs大气沉降峰值叠加，共同形成柱状样2.7 m处的最大蓄积峰；1967年137Cs大气沉降量下降但河流入海泥沙量达最大值，形成柱状样1.9 m处的次级蓄积峰。
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图 5 1964—1976年黄河输沙量的年际变化图Figure 5. Interannual variation of sediment discharge of the Yellow River from 1964 to 19763.3 研究区沉积环境演变的粒度与核素证据
黄河入海口的变迁导致研究区沉积环境在三角洲侧缘和海岸沉积环境间转变，而这种变化在沉积物粒度、210Pbex活度分布以及137Cs活度分布上均有表现（图2）。1964年前（黄河未从刁口流路入海）研究区沉积环境稳定，沉积物无黄河输沙来源，因此柱状样K2下部的沉积物粒度组分变化稳定；此时核素主要为大气沉降来源，137Cs与210Pbex均遵守核素分布规律，210Pbex活度剖面在深度1.9～3.5 m呈现理想的衰变形式，这与李凤业研究的210Pb混合区—衰变区—本底区的阶段式分布结论相符[11]，由于柱状样长度的限制，研究区并未出现本底层。1964年，黄河携带大量泥沙由刁口流路入海，研究区沉积物来源于黄河入海泥沙且堆积速度很快，此时137Cs除大气沉降外还存在流域输入来源，两者共同作用形成2.7m处的最大蓄积峰。1967年（柱状样1.9 m处），黄河入海泥沙量最大，137Cs活度出现次级蓄积峰值，这时210Pbex活度与沉积物中砂粒含量均达到最大值。沉积物粒度组分的突变为2.1 m处，未与137Cs最大蓄积峰（2.7 m）相对应，本文推测可能由两点原因造成：（1）黄河入海泥沙的2/3堆积在口门处，河流改道初期研究区泥沙来量相对较小，随着岸线的不断推移,研究区泥沙堆积不断增多，而后沉积物粒度组分发生变化。（2）黄河所携泥沙中以粉砂为主，占55%～88%，砂占7%～34%，与研究区底质沉积物类型有较高一致性，因此在改道初期沉积物粒度组分变化不大，后由于黄河泥沙与水动力的改变造成沉积物粒度组分的突变。1976年（黄河改道清水沟）后，研究区缺少入海泥沙供应，沉积环境极不稳定，波浪、潮流和潮汐等成为本区的主要动力作用，研究区遭受冲刷与侵蚀作用且沉积物的再悬浮与再沉积现象显著，沉积物粒径较1964—1976年小幅度下降，但仍比1964年前大。柱状样K2在0～1.9 m（1967年）先后经历沉积物的快速堆积与侵蚀，因此 210Pbex表现为混合层。
综上所述，本文将柱状样K2的深度2.7 m处定为1964年，深度1.9 m处定为1967年；因此推断研究区1964—1967年沉积物淤积厚度为0.8 m，这一结果与统计的历史水深数据相符。柱状样K2的沉积物砂粒含量在1.9 m处的最大值、137Cs活度剖面1.9 m处的次级蓄积峰与210Pbex活度分布以1.9 m为界的阶段式划分均记录了黄河改道由刁口入海并在1967年达到入海泥沙量最大值的过程。
4. 结论
（1）柱状样K2的137Cs活度剖面存在两个蓄积峰值，最大蓄积峰值（2.7 m处）对应于1964年，次级蓄积峰（1.9 m处）对应于1967年。在沉积环境不稳定区域可结合事件性沉积或其他测年手段进行137Cs的辅助定年。
（2）柱状样K2的210Pbex呈现明显的两段式分布，这种分布方式与黄河口变迁及沉积物来源的变化相关。1967年前，研究区沉积环境较稳定、泥沙来源单一并在1967年达到最大值，210Pbex表现为衰变层；1967年后，研究区沉积环境复杂，沉积物经历了先堆积后侵蚀， 210Pbex表现为混合层。
（3）黄河口变迁造成研究区沉积环境的演变在137Cs活度、沉积物粒度与210Pbex活度的分布上均有表现。虽然黄河改道清水沟后本区遭受侵蚀作用，但侵蚀厚度远低于淤积厚度，且1964年（黄河改道清水沟）前的沉积物未遭受侵蚀。
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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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