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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作为我国东部陆架海，渤、黄海因其复杂的海洋动力学特征、丰富的沉积物来源一直以来都是国内外海洋学者研究的重点区域。唐山港位于渤海湾和辽东湾之间的交界处，靠近渤海湾北部的海岸带一侧[1-2]，其南部为走向近EW向的曹妃甸深槽，是渤海湾最深的水域。该区海陆相互作用频繁，发育沙质海岸和泥质海岸，第四纪沉积演化过程十分复杂，再加上近年来开展的围填海工程导致潮流系统和滩海地貌发生巨大变化[1]，严重影响了唐山港及其周边海域的沉积环境。前人在渤海湾唐山港及其附近海域开展了大量的研究工作，主要集中在海侵过程[3-5]、海平面变化与海岸变迁[2, 6]、潮流通道变化[7]以及第四纪沉积演化等方面[3, 8]，而对于该区沉积物沉积过程与搬运机制等学者较为关注的问题的研究则相对有限。
河流物质的输入是海底沉积物的重要来源[9-10]，渤海湾三面环陆，入海河流众多，有清河、海河、蓟运河、黄河、辽河以及滦河等。其中，海河、黄河以及滦河是渤海湾西部地区沿岸径流量相对较大的3条河流，是该区最主要的沉积物来源。前人通过元素地球化学、黏土矿物等方法对渤海湾西岸的沉积物源进行了示踪[11-14]，但目前针对渤海湾西缘表层沉积物的来源研究仍存在争议，主要存在以下两种观点：一种观点认为渤海湾西缘唐山港附近靠近海河入海口，沉积物主要是海河来源的陆源碎屑物质[13]，可能部分也受到滦河的影响[15]；另一种观点则认为由于受到渤海湾环流的影响，唐山港附近海域主要是黄河-海河混合来源的陆源碎屑物质[11-12, 14]。唐山港附近海域是否有黄河和滦河来源物质的加入，黄河携带的物质在渤海湾地区的分布范围及特征等问题尚未解决。因此，渤海湾西缘唐山港附近海域沉积物来源问题亟需可靠的物源指标来进一步的分析和研究。
沉积物粒度受物源区性质、沉积作用以及沉积动力学过程等多种因素影响，导致不同沉积环境中沉积物粒度特征明显不同，因此常被用来作为判断沉积物来源、水动力条件以及重建古气候和古环境演化的重要参数，广泛应用于海洋、河流以及湖泊沉积环境的研究中[13, 16]。黏土矿物是地表母岩经风化作用形成的产物，是海洋陆源碎屑中重要的组成成分，是示踪海洋沉积物来源以及指示沉积环境演化等内容的重要指标[17-19]。本文通过对研究区沉积物粒度、黏土矿物等指标开展测试分析，同时与周围河流输运的沉积物中粒度和黏土矿物特征进行对比，以期揭示渤海湾唐山港海域附近表层沉积物粒度和黏土矿物分布特征，初步探讨渤海湾西缘现代沉积物物质来源及其控制因素。
1. 区域地质背景
唐山港位于渤海湾北部唐山市东南部沿海，包含京唐港区和曹妃甸港区。唐山港海域水深较浅，平均水深18 m，最大水深为36 m，位于研究区曹妃甸深槽处（图1）。曹妃甸深槽走向近EW向，沟槽北陡南缓，是在地质构造和水下河谷的双重作用下发育形成的[1]，是全新世滦河向海输送泥沙的入海处[20]，岬角地貌和特殊地形特征使得附近海域水动力增强，对深槽冲刷作用较为严重，是深槽长期维持水深的重要因素[1]。研究区地形和地貌类型较为复杂，内侧为古滦河三角洲发育的冲积-海积平原，外侧为曹妃甸-东坑坨沙质岸线[1]。深槽附近的地貌自西向东可划分为南堡海岸地貌、曹妃甸深槽和老龙沟潟湖3个体系单元[1, 21]。近年来由于大规模的围填海工程，深槽附近出现了新的侵蚀洼地和海底滑塌等地貌类型。从曹妃甸向渤海海峡有条27 m深的天然水道，深槽和水道使得唐山港具备成为渤海沿岸的大型泊位港址的天然优势。
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图 1 渤海湾唐山港海域表层沉积物取样站位及海流示意图Figure 1. Surface sediment sampling stations and currents in Tangshan Harbor, Bohai Bay黄河是中国第二大河流，平均径流量为3.16×1010 m3/a，约占渤海河流输入的90%，每年向边缘海输送约1.4×108 t的沉积物[22]，其中30%～40%的沉积物堆积在河口处[23]，其搬运的物质覆盖渤海湾、渤海海峡南部以及莱州湾以北的渤中海域，是渤海湾最主要的沉积物来源[24]。海河的平均径流量为2.15×1010 m3/a[25]，输沙量约 6.0×106 t/a[14]。虽然蓟运河的径流量和输沙量远小于海河，但对渤海湾地区沉积物也有一定的贡献。滦河平均径流量为4.6×109 m3/a，平均输沙量约为 2.0×107 t/a，沉积物相对较粗，主要是沉积在滦河河口到曹妃甸沿岸区域[26]。
渤海环流体系主要是由渤海沿岸流和外海来的黄海暖流余脉组成，具有北进南出的特征（图1a）。冬季黄海暖流余脉流自渤海海峡北部进入渤海并延伸至渤海西岸，同时由于受到沿岸的阻挡导致其分为南北两支，其中南支在进入渤海湾后沿岸转折南下，流经莱州湾后从渤海海峡逆时针方向流出渤海；北支则是沿着辽东湾西岸向北运移，与辽东湾低盐水的沿岸流形成顺时针环流[24, 27]。渤海沿岸流和黄海暖流共同构成渤海南部顺时针、北部逆时针方向的双环流体系结构[24, 27-28]。夏季的环流流型与冬季相近，也是北部顺时针、南部逆时针的双环流结构，除了黄海暖流产生的北向分支，会沿着辽东湾东岸北上。渤海潮流以半日潮流为主，流速0.5～1.0 m/s，老铁山水道附近潮流最强为1.5～2.0 m/s[27]。渤海潮余流从黄河三角洲向北-东北方向流动，受辽东湾西岸阻隔向右转向，沿着辽东湾沿岸向辽东半岛南部流动，在渤海中部和辽东湾附近形成顺时针的余环流[27]，对渤海湾中部环流具有重要的贡献。
2. 材料与方法
2.1 样品来源
2021年中国地质调查局烟台海岸带地质调查中心依托中国地质调查局1∶5万海洋区域地质调查项目对渤海湾曹妃甸地区进行表层沉积物系统取样（图1b）。参照《海洋区域地质调查规范（1∶50000）》（DZ/T 0255-2014），取样站位按照1 km×1 km网格间距进行设计，利用抓斗取样器采集0～2 cm表层沉积物。取回的沉积物被放置在密封的无菌袋中，并4℃避光储存。
2.2 测试方法
取0.5 g的样品于离心管中，加入30%的H2O2和10%的HCl去除沉积物中的有机质和碳酸盐。上机前加入0.5 M的六偏磷酸钠（NaPO3）6并经超声波完全分散，利用奥地利Anton Paar PSA1190激光粒度分析仪进行粒度分析测试，仪器的测量范围为0.04～2500 μm，同一样品进行两次平行测量，重复测量相对误差＜1%[31]，分析测试精度＜3%。表层沉积物粒度数据由中国地质调查局烟台海岸带地质调查中心项目组提供[31]，部分数据已发表。粒度参数的计算和等级划分采用Folk和Ward分类方案[32]，依据粒径＜4 μm、4～63 μm和＞63 μm将粒度分为黏土、粉砂和砂[33]。
黏土矿物分析测试采用X射线衍射方法（X-ray Diffraction, XRD）在中国海洋大学海洋地球科学学院黏土矿物分析实验室完成。取适量样品于离心管中，加入少量10%的过氧化氢溶液以除去沉积物中的有机质，然后加纯水离心清洗三次，后再加入50%的醋酸以除去沉积物中的碳酸盐，再用水将样品洗至中性。取上层浊液于离心管中加入2滴饱和NaCl溶液，利用Stoke沉降原理提取出粒度小于2 μm的悬浮液，制成涂片自然风干后用乙二醇蒸汽饱和制成乙二醇饱和片[34]，将其置于德国布鲁克AXS公司生产的Bruker D8 ADVANCE型X射线衍射仪中进行测试分析，仪器分析参数为Cu 靶、管电压 40 kv、管电流 80 mA、扫描范围3°～30°（2θ）、扫描步进长度（2θ）0.02°，仪器峰位精度≤0.01°2θ。依据Biscaye[18]方法选取乙二醇饱和片图谱上的蒙脱石（17 Å, （1 Å=10–10 m））、伊利石（10 Å）、绿泥石（7 Å）和高岭石（7 Å）4种黏度矿物的3个特征衍射峰的峰面积为基础数据进行计算，按照1∶4∶2的权重因子换算获得蒙脱石、伊利石、绿泥石和高岭石的相对含量。随后以25°（2θ）左右3.5 Å 附近的衍射峰高比值换算获得高岭石（3.57 Å）和绿泥石（3.53 Å）的相对含量。经均一化处理4种黏土矿物的总含量为100%。为保证实验结果的准确性，实验过程中每批样品设置10 %平行样，平行样合格率为100%。
3. 结果
3.1 粒度分布特征
3.1.1 粒级组分分布特征
分析结果表明，渤海湾唐山港附近海域表层沉积物主要是由粉砂质砂（zS）、砂质粉砂（sZ）、粉砂（Z）以及少量的砂（S）和黏土等组成（图2）[31]。黏土粒级组分相对含量为0.52%～51.11%，平均含量为21.45%；粉砂粒级组分含量为0.87%～79.05%，平均含量为50.38%；砂质粒级组分含量为0～98.61%，平均含量为28.17%。根据粒度组成特征，以砂含量65%和25%等值线作为划分的标准，将研究区可以划分为3个区域，研究区东北部以砂和粉砂质砂为主，沉积物颗粒偏粗；唐山港海域曹妃甸深槽处以砂质粉砂和粉砂质砂为主；南部和唐山港附近区域沉积物粒度相对偏细，主要以粉砂为主（图3b-d）。
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图 2 渤海湾唐山港海域表层沉积物三角分类图S-砂，C-黏土，M-泥，Z-粉砂，sC-砂质黏土，sM-砂质泥，sZ-砂质粉砂，cS-黏土质砂，mS-泥质砂，zS-粉砂质砂。Figure 2. Ternary classification of surface sediments in Tangshan Harbor, Bohai BayS-sand, C-clay, M-mud, Z-silt, sC-sandy clay, sM-sandy mud, sZ-sandy silt, cS-clayey sand, mS-muddy sand, zS-silty sand.![]()
图 3 渤海湾唐山港海域水深和表层沉积物粒度分布图a：水深，b：黏土，c：粉砂，d：砂。Figure 3. Bathymetric map and the distribution patterns of grain size of surface sediments in Tangshan Harbor, Bohai Baya: Water depth, b: clay, c: silt, d: sand.3.1.2 粒度参数分布特征
渤海湾唐山港附近海域表层沉积物平均粒径（Mz）为1.4～7.71 Φ，平均值为5.72 Φ，整体沉积物粒度中等偏粗。研究区东北部由沿岸向海（由北向南）沉积物粒度整体呈现出逐渐变细的趋势（图4a）。粒度分选系数变化δ值为0.67～2.91，平均值为2.0，绝大部分沉积物属于分选较差—差。研究区东北部和中部曹妃甸深槽区δ值为2～3，分选系数较高；南部和唐山港附近海域分选系数较低，δ值一般小于2（图4b）。表层沉积物粒度偏态Sk为–0.22～0.72，平均值为0.33，绝大多数属于正偏。研究区东北部和中部曹妃甸深槽处为偏度高值区，Sk为0.6～0.72；南部和唐山港附近海域附近Sk值均小于0.2，为负偏态（图4c）。粒度峰态Ku变化范围为0.66～2.36，平均值为0.98，除了研究区东部局部区域出现很尖锐峰态外，整体变化不大，为中等峰态（图4d）。
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图 4 渤海湾唐山港海域表层沉积物粒度参数分布图a：平均粒径，b：分选系数，c：偏态，d：峰态。Figure 4. Distribution patterns of grain size parameters of surface sediments in Tangshan Harbor, Bohai Baya: Mean grain size, b: sorting coefficient, c: skewness, d: kurtosis.3.2 粒度端元分析
利用粒度端元模型（End-member modelling analysis，EMMA）计算研究区表层沉积物粒度端元值，复相关系数（R2）代表粒度实测数据被端元拟合的程度[35]。为较好地获取拟合粒度数据的最小端元数，假设端元数是2～10的情况下，对各粒级复相关系数和所有粒级复相关系数平均值进行计算。结果显示端元数为2、3时，平均复相关系数分别为0.85和0.90（图5a），但26～125 μm拟合程度较差，不能满足粒级拟合的需要。当端元数为4时，大部分粒级拟合程度大于0.8，平均复相关系数为0.95（图5a），说明4个端元满足拟合的需要。根据端元分析方法选取端元应遵循尽量少的原则[36]，选取4个端元（EM1—EM4）对该区粒度数据进行拟合。
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图 5 渤海湾唐山港海域表层沉积物粒度端元分析结果a：粒度端元数-复相关系数平均值，b：4个端元（EM1-EM4）粒度频率分布曲线。Figure 5. End-member analysis of surface sediments in Tangshan Harbor, Bohai Baya: End member-mean coefficient of determination, b: frequency curves of four end-members (EM1-EM4).端元粒度频率分布曲线显示4个端元中EM1、EM2和EM4都具有一个明显的主峰，分布形态接近正态分布，EM1到EM4 粒径增大，分选变好（图5b）。端元EM1粒径众数值为10 μm，为细粉砂；EM2粒径众数值为20 μm，为中粉砂；EM3粒径众数值为200 μm，为中砂，在细颗粒组分6～7 μm处可见次峰，为细砂。端元EM4粒径众数值为300 μm，为粗砂（图5b）。
在沉积物粒度4端元相对含量平面等值线图上，EM1含量为0～97.77%，平均含量为22.28%，在研究区均有分布，高值区主要是在研究区西部靠近海河区域，并有从近岸向外海方向递减的趋势（图6a）。EM2含量为0～100%，平均含量为19.60%，在渤海湾全区均有分布，主要集中在唐山港附近海域，并有从近岸向外海方向递减的趋势（图6b）。EM3含量为0～74.07%，平均含量为28.77%，主要分布在研究区东北部、北部以及中部曹妃甸深槽区域（图6c）。EM4含量为0～72.58%，平均含量为29.34%，主要分布在中部曹妃甸深槽区域（图6d）。
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图 6 渤海湾唐山港海域表层沉积物4个端元相对含量平面分布Figure 6. Distribution of relative contents of four end-members of surface sediments in Tangshan Harbor, Bohai Bay3.3 黏土矿物分布特征
渤海湾唐山港附近海域表层沉积物中黏土矿物主要是由大量的伊利石（66%～86%，平均含量72%）、少量的蒙脱石（2%～18%，平均含量12%）、绿泥石（4%～11%，平均含量8%）以及高岭石（5%～15%，平均含量8%）组成。唐山港附近伊利石含量相对较高（75%以上），蒙脱石含量12%左右，而高岭石、绿泥石含量相对较低，为6%左右（图7）。研究区东北部为蒙脱石相对高值区，伊利石、高岭石以及绿泥石低值区；曹妃甸深槽处则出现蒙脱石、高岭石以及绿泥石相对高值区、伊利石低值区；南区域总体呈现出蒙脱石和高岭石相对高值区、伊利石和绿泥石相对低值区，局部存在蒙脱石和高岭石相对低值区、伊利石和绿泥石的局部高值区；唐山港海域附近则整体表现为蒙脱石和伊利石相对高值区、高岭石和绿泥石的相对低值区（图7）。
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图 7 渤海湾唐山港海域表层沉积物黏土矿物相对含量分布图Figure 7. Distribution of the relative content of clay minerals in surface sediments in Tangshan Harbor, Bohai Bay4. 讨论
4.1 物源判别
渤海沉积物来源主要是河流作用携带的陆源碎屑物质、外海物质、大气沉降物质以及周围基岩侵蚀风化形成的物质[10, 24]。其中，渤海湾周围河流入海物质贡献量较大，占渤海沉积物的90%左右，以黄河、海河和滦河等为主。了解沉积物潜在物源区和迁移过程是进行物源判别的前提[19, 37]。尽管中国大陆的风尘颗粒在太平洋深海碎屑物质通量中贡献较大[38-39]，但在大陆边缘海沉积物中风尘物质含量较低，大量河流来源的碎屑物质将风尘物质信息掩盖[40]，可忽略不计。
由于受到流域气候条件的影响，不同来源沉积物中粒度和黏土矿物相对含量具有明显的差别（表1）。滦河平均年输沙量20.1 Mt，流经中酸性的岩浆岩、古中新生代的砂页岩和灰岩等沉积岩以及前古生代变质岩的蚀变源区[41]，沉积物粒度相对较粗，主要是中细砂等粗粒级为主，细粒级的物质相对较少。黏土矿物呈现出伊利石含量相对较低而高岭石+绿泥石、蒙脱石含量相对较高的特征；海河沉积物粒度较细，主要是以黏土质粉砂为主[42]。沉积物中黏土矿物含量特征则与滦河相反，呈现出伊利石含量相对较高、而蒙脱石和高岭石+绿泥石含量较低的特征；黄河流经黄土高原，携带大量的泥沙入海，每年大概2/3的泥沙沉积物堆积在黄河三角洲地区，其余的则被带到三角洲滨海区外[41]。其沉积物颗粒主要是由黏土质粉砂和少量的黏土组成，粒度相对较细[42]，黏土矿物含量则介于海河与滦河之间，且更接近于海河[42]（表1）。
表 1 渤海湾唐山港附近海域及周围河流表层沉积物中黏土矿物相对含量Table 1. Relative content of clay minerals in surface sediments of the Tangshan Harbor and surrounding rivers in the Bohai Bay样品位置 样品数量/个 蒙脱石/% 伊利石/% 高岭石/% 绿泥石/% 伊利石结晶度 数据来源 唐山港海域 161 12 72 8 8 0.43 本文 HH-1 23.0 58.0 12.0 7.0 引自文献[43] HH-2 23.2 59.0 8.5 9.3 引自文献[44] HH-3 13.0 67.0 8.0 12.0 引自文献[45] HH-4 16.0 62.0 10.0 12.0 引自文献[46] HH-5 15.2 62.5 9.7 12.5 引自文献[47] HH-6 10.0 60.0 12.0 18.0 引自文献[48] HH-7 12.0 62.0 10.0 16.0 引自文献[49] HH-8 21.0 61.0 9.0 9.0 引自文献[42] HH-9 16 29 (11～44) 54 (39～69) 7 (5～9) 10 (9～14) 0.33 引自文献[50] LR-1 22 48 16 14 0.45 引自文献[19] LR-2 15 54 16 16 0.43 LR-3 24 46 16 14 0.47 LR-4 27 50 12 12 0.48 LR-5 26 47 14 13 0.43 HR-1 7 63 14 19 0.36 引自文献[19] HR-2 9 64 14 14 0.35 注：HH1-9: 黄河表层沉积物中黏土矿物；LR1-5: 滦河表层沉积物中黏土矿物；HR1-2: 海河表层沉积物中黏土矿物。 为确定渤海湾物源区，利用粒度组分、蒙脱石-（伊利石+绿泥石）-高岭石三角图和高岭石/绿泥石-伊利石/蒙脱石的比值进行判别（图8a-b），并与周围潜在的河流沉积物中黏土矿物相对含量进行对比分析，发现唐山港海域表层沉积物黏土矿物主要落在黄河和海河之间的区域，指示细颗粒沉积物主要来源于黄河-海河混合的陆源碎屑物质。这与粒度端元组分EM1在研究区均有分布，并由近岸向外海方向递减的趋势相一致（图6a），代表悬浮搬运的现代陆源细颗粒物质，因此认为细颗粒沉积物来源主要是黄河-海河混合的陆源碎屑物质，与前人的研究较为一致[11-12, 14]。此外，粒度分布特征显示研究区东北部和唐山港南部曹妃甸深槽处对应的沉积物类型主要是粉砂质砂和砂质粉砂，粒度相对偏粗（图4a），而海河径流输入泥沙中值粒径为5～20 μm，颗粒很细，黄河来源的物质主要是黏土质粉砂，粒度也相对较细[42]，如果只依靠来自海河和黄河携带的泥沙供应无法形成粉砂质砂等较粗的沉积物类型，因而对于研究区东北部和中部曹妃甸深槽区粗颗粒沉积物来源问题，还需要结合粒度特征对沉积物做进一步的物源分析。李从先等研究认为唐山港曹妃甸海区位于古滦河三角洲的发育区[20]，全新世晚期以来由于海平面下降，滦河改道向北迁移，泥沙供应不足才导致三角洲停止发育，使得该区处于废弃的三角洲沉积环境[1]。因此，我们认为曹妃甸深槽区还可能有部分古滦河物质的加入[15]。
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图 8 渤海湾唐山港附近海域及周围河流表层沉积物黏土矿物组合三角图和比值散点图a：黏土组合蒙脱石-(伊利石+绿泥石)-高岭石三角图，b：伊利石/蒙脱石-高岭石/绿泥石比值散点图；HH-黄河；LR-滦河；HR-海河。Figure 8. Triangle and scatter diagram of the clay minerals of surface sediments in Tangshan Harbor and surrounding riversa: Triangle diagram of clay minerals assemblages smectite-(illite+chlorite)-kaolinite, b: Scatter plot of illite/smectite-kaolinite/chlorite ratios; HH-Yellow River; LR-Luan River; HR-Hai River.4.2 沉积动力环境分析
沉积物粒度数据保存大量与沉积物输运和沉降有关的信息，可以揭示研究区水动力特征以及沉积物输运过程。粒度端元EM1对应沉积物类型主要是细粉砂，一般对应弱的潮流场，在唐山港西部出现高值区，且含量自沿岸向渤海湾逐渐递减（图6a），与该区的潮流走向[27]大致相当，代表了形成现代泥质沉积区的动力组分；粒度端元EM2在研究区北部存在高值区，且向中部曹妃甸深槽处呈现出逐渐减少的趋势（图6b），对应沉积物类型主要是砂质粉砂、中粉砂，可能代表水动力条件中等；粒度端元EM3主要分布在研究区东北部和中部曹妃甸深槽（图6c）；端元EM4高值区有中部曹妃甸深槽和北部部分区域，分别对应的沉积物类型为粉砂质砂和砂，代表该区域水动力环境较强（图6d）。
除了受沉积物物源的影响外，渤海湾唐山港海域表层沉积物的粒度和黏土矿物分布特征还大致与渤海湾的环流体系和潮流场密切相关[10, 14, 24]，显示出潮流场对黄河、滦河以及海河物质的搬运和扩散影响[27, 51]。夏季波浪作用相对较弱，黄河、海河以及滦河入海沉积物绝大部分沉积在河口处，少部分通过环流向远端扩散迁移沉积。冬季风浪较强，沉积在河口三角洲处的沉积物在海流和波浪作用下，发生侵蚀再悬浮作用向远端扩散迁移。根据渤海湾潮余流数值动力学模型[52]，潮余流沿渤海湾北岸的滦河口附近流向唐山港东北部，然后一分为二，分为洋流A和洋流B两条路线。洋流A通过港口时流速减慢，使得悬浮颗粒物质沉积。进入研究区域后，洋流B转向东南，呈逆时针方向环流，随后悬浮的细颗粒沉积物在港口东南部沉积。洋流A从研究区域流出在天津塘沽北部永定新河河口附近分为两股，一条分支洋流C，携带着海河河口沉积物沿着海岸向北进入渤海湾西北部海域，沿岸河流中的悬浮细颗粒物质由于流速降低，沉积在港口西部。另一股洋流D沿西部海岸向南移动到南部海岸，然后沿南部海岸向东移动，其中一部分可能向北进入研究区。黄河中的泥沙入海后其沉积物在渤海环流的作用下向东北、东南和西北3个方向扩散[53]，其中向东北方向迁移的环流和洋流D共同作用将黄河细颗粒沉积物迁移至研究区。洋流C和洋流D在港口附近与洋流A汇合，使得研究区细颗粒组分主要是海河-黄河混合的沉积物质。此外，少量的滦河三角洲（包括古滦河三角洲）入海泥砂和粗颗粒物质在渤海湾反时针环流和波浪的共同作用下由滦河口北部沿岸向研究区东北部和中部曹妃甸深槽搬运沉积（图9），形成曹妃甸的离岸沙坝。渤海湾唐山港海域受到环流和潮流体系的影响，接受来自周围的黄河-海河物质以及部分的滦河物质的供应。
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图 9 渤海湾唐山港附近沉积物迁移模式图Figure 9. Sediment transport pattern in Tangshan Harbor area, Bohai Bay5. 结论
（1） 唐山港海域表层沉积物有5种类型，主要以粉砂质砂和砂质粉砂为主。各组分中以粉砂含量最高，平均值为50.38%，其次是砂，平均含量为28.17%，黏土含量最低，平均含量为21.45%。
（2） 根据粒度参数特征，研究区大致可以分为3个区：东北部以粉砂质砂为主，分选较差，正偏态；中部曹妃甸深槽区以砂质粉砂为主，分选差，正偏态；南部和西北部以粉砂为主，分选中等—较差。
（3） 粒度端元模型显示，唐山港海域表层沉积物粒度可分离EM1—EM4四个端元，其众数值分别为10、20、200和300 μm，平均含量分别为22.28%、19.60%、28.77%和29.34%。EM1和EM2反映了沉积动力环境弱，EM3和EM4则反映沉积动力环境强，可能会对沉积物冲刷改造。
（4） 利用蒙脱石-（伊利石+绿泥石）-高岭石矿物组合和高岭石/绿泥石-伊利石/蒙脱石比值识别出沉积物细颗粒组分来源主要是黄河-海河混合的陆源碎屑物质。曹妃甸深槽区可能有部分古滦河三角洲粗颗粒物质的加入。
（5） 渤海环流和潮余流控制着本区细颗粒沉积物主要向南部和唐山港附近迁移沉积，粗颗粒物质向东北部和中部曹妃甸区搬运沉积。
致谢：衷心感谢编辑和审稿专家在论文修改过程中的指导和帮助，感谢渤海曹妃甸海域1∶5万海洋区域地质调查的全体出海人员采集的表层沉积物样品。
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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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