Rethinking on shallow sedimentary sequence and its evolution of the Xiyang tidal channel in the Radial Sand Ridge Field, South Yellow Sea
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摘要: 晚第四纪以来，黄河、长江都曾经江苏中部海岸注入南黄海，河海交互作用形成一系列沉积，全新世海侵后发育岸外辐射沙脊群。沙脊群西北部、由岸滩与沙脊所夹持的西洋潮流通道，位于北侧废黄河三角洲和南侧长江三角洲两大地貌单元间的过渡区，成为揭示不同大河交互作用下的海岸、陆架晚第四纪沉积层序模式的重要窗口。最近通过更多晚第四纪钻孔对比和浅层地震剖面集成研究发现：① 由于混乱的测年结果和陆相硬黏土层对比不当，造成之前基于07SR01孔和Y1孔构建的辐射沙脊群西洋潮流通道浅部沉积（标高−60 m以内）的年代框架有误，其主体应是晚更新世沉积且发育两个沉积旋回，末次冰盛期硬黏土层多被潮流侵蚀而缺失，表层全新世沉积厚度在水下沙脊处基本不足10 m，其余普遍不足5 m，甚至缺失；② 仅在西洋西北段稳定分布的浅层地震单元U3指示了MIS 3古黄河三角洲的南缘，自晚更新世以来西洋所在的江苏中部海岸可能深受古黄河物源的影响，这尚需在西洋西北段的关键位置钻取新孔，并结合已有浅层地震剖面和东南段钻孔来进一步研究证实。提出下一步工作将基于层序地层学方法，通过对已有控制性浅层地震剖面进行地震层序格架的三维可视化、提取地震单元和反射界面的空间分布特征，结合已有及新增控制性钻孔的沉积学和年代学研究，构建可靠年代框架、判识大河物源，并参考邻区钻孔资料，来探明西洋潮流通道的浅部沉积层序，反演其形成演化。Abstract: Since the Late Quaternary, both the Yellow River and Changjiang River entered into the South Yellow Sea flowing through the middle Jiangsu coast. As a result, a series of sediments have been deposited in this area controlled by the river-sea interactions. The Radial Sand Ridge Field (RSRF) off the middle Jiangsu coast has been formed after the Holocene transgression. The Xiyang tidal channel in the northwestern RSRF is constrained by the tidal flat coast and tidal ridges. It is located in the transition zone between the northern Abandoned Yellow River delta and southern modern Changjiang River delta. Therefore, it becomes the important window area to reveal the sedimentary sequence formed in the coast and continental shelf under the active interactions between different large rivers during the Late Quaternary. As to the upper strata with the depth less than 60 m below the current mean sea-level in the Xiyang tidal channel, there are still different viewpoints on its sedimentary sequence, chronology framework and evolution, while the concerned studies are still pretty limited. Recently, the results of further Late Quaternary stratigraphic correlations and synthesis study on shallow seismic profiles showed that, (1) Due to disordered dating results and improper correlation of terrigenous stiff mud layers, the chronology framework of Xiyang upper strata built previously based on core 07SR01 and Y1 is incorrect, the main part of the upper strata including two sedimentary cycles are the Late Pleistocene deposits and the stiff mud layer of the Last Glacial Maximum is often missing due to the tidal scouring, the thickness of surficial Holocene sediments are generally less than 10 m in the submerged sand ridges, and extensively less than 5 m in other places, or even zero in some places; (2) The shallow seismic unit 3 (U3) only steadily located in the northwestern part of the Xiyang tidal channel indicates the southern margin of the old Yellow River delta developed during MIS 3, and the middle Jiangsu coast in which the Xiyang tidal channel is located was probably influenced deeply by the old Yellow River sediments since the Late Pleistocene, however it is still necessary to recover a new sedimentary core in the key position of northwestern part, plus further study and verification based on the new core and other acquired shallow seismic profiles and cores in the southeastern part should be done. Thus, this paper proposed the further study plan as follows, based on the 3D visualization of the seismic sequence framework, the spatial characteristics of the seismic units and main reflection interfaces would be extracted. Furthermore, combined with the sedimentology and chronology studies of the existing and designed cores, the reliable chronology framework would be set up expectedly, and the provenance from large rivers would be identified. Applying the sequence stratigraphy method, referencing the adjacent published core data, it is targeted to ascertain the shallow sedimentary sequence in the Xiyang tidal channel, and to reveal its evolution.
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断裂是含油气盆地的重要研究对象，控制着盆地结构与演化过程，同时与圈闭的形成、分布以及油气运聚过程等关键成藏要素密切相关[1-7]。而油气成藏模式是对油气藏特征、形成过程等多要素的总结，综合各主控因素建立动态成藏过程，对有利目标勘探具有重要指导意义[8-9]。
陆丰凹陷是珠江口盆地珠I坳陷内的一个富油凹陷，近年来在陆丰凹陷南部地区取得多个重要油气勘探突破[10-12]。前人对陆丰凹陷的构造演化、沉积充填及油气成藏等方面均开展过详细研究，并取得一定成果[13-18]。随着勘探的深入及新油田的不断发现，研究区的基础资料逐渐丰富，但仍存在较多问题，如断裂输导能力的强弱、油气运移路径及运聚效率等因素尚不明确，从而导致油气成藏要素相似、构造位置相邻的钻井勘探成效经常存在较大差别[10, 15]。因此需要对已有的成果认识不断总结完善，对油气成藏的控制因素也需要进一步深化。本文在充分吸收前人研究成果的基础上，以断裂和油气成藏为两个主要研究目标，结合陆丰凹陷南部的最新三维地震解释成果及钻井资料，对陆丰凹陷南部的断裂开展几何学及运动学研究，明确断裂发育特征及其演化过程，并探究断裂对油气运聚成藏的控制作用，总结油气成藏模式，为该地区油气勘探提供理论依据。
1. 区域地质概况
珠江口盆地位于南海北部陆缘，整体发育NE向展布的坳隆相间结构，自北向南包括北部隆起带、北部坳陷带、中央隆起带、南部坳陷带和南部隆起带（图1a）。陆丰凹陷位于珠江口盆地北部坳陷带的珠I坳陷内，南至东沙隆起，北至北部隆起，西接惠陆低凸起，东接海丰凸起。陆丰凹陷内发育多个次级洼陷，其中南部地区发育陆丰13西洼、陆丰13东洼和陆丰15洼（图1b）。
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图 1 陆丰凹陷南部构造位置及主要断裂分布Figure 1. Tectonic location and distribution of main faults in the southern Lufeng Sag陆丰凹陷在新生代经历了多期构造演化，始新世为裂陷演化阶段，主要沉积文昌组和恩平组，各洼陷在该时期也基本形成；渐新世—新近纪转变为拗陷演化阶段，构造活动微弱，沉积了珠海组、珠江组、韩江组、粤海组和万山组，沉积环境也随之由陆相转变为海相（图2）。珠琼运动I幕使陆丰凹陷遭受强烈伸展作用，南部地区的控洼断裂发生强烈活动，形成了欠补偿的沉积环境，洼陷内快速沉积较厚的半深湖-深湖相暗色泥岩，成为该地区的主力烃源岩[13, 19-20]，其中，文昌组烃源岩TOC约为0.6%～7.7%，R0值为0.7%～1.2%，生烃潜力较好[10, 21-22]。陆丰凹陷油气大规模成藏期为新近系韩江组沉积期[11, 19]。
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图 2 陆丰凹陷地层综合柱状图Figure 2. Correlation of stratigraphic, sedimentary, and tectonic histogram of the Lufeng sag2. 断裂发育特征
2.1 剖面变形特征
依据断裂规模、活动强度及对沉积的控制作用等，可将陆丰凹陷南部地区的断裂划分为3个级别。一级断裂为控洼边界断裂，活动性强，主要包括陆丰13西断层、陆丰13东断层和陆丰15断层（分别对应图1中的F1、F2和F3）；二级断裂活动性弱于一级断裂，主要控制洼陷内局部构造带的形成演化；三级断裂数量多分布广，多为单期活动且活动性较弱，其形成演化受控于一级或二级断裂。
陆丰13西断层（F1）为近铲式形态的南倾正断层，断层向下断穿至基底，向上终止于韩江组（图3a）。陆丰13西断层在古近纪持续活动，使陆丰13西洼呈北断南超的楔形结构。断裂在新近纪发生微弱活动，并不再控制洼陷结构特征。陆丰13西洼的生长地层厚度由下文昌组向上至恩平组逐渐增厚，反映了由裂陷I幕至裂陷II幕，陆丰13西断层的活动性逐渐增强。洼陷内三级断裂发育较少，以南倾板式正断层为主，多分布于文昌组内，以多米诺式断层组合富集于陆丰13斜坡带。
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图 3 陆丰凹陷南部洼陷结构及断裂发育特征剖面位置见图1b。Figure 3. Characteristics of geological structure and faults development in the southern Lufeng SagThe section location is seen in Fig.1b.陆丰13东断层（F2）为近铲式形态的低倾角南倾正断层，断层向下断穿至基底，向上终止于珠江组内（图3b）。陆丰13东断层在文昌组沉积期强烈活动，控制着洼陷北断南超半地堑的形成，至恩平组沉积期断层活动性逐渐减弱，断层两盘地层厚度差异明显减小（图3b）。陆丰13东洼内三级断裂发育较多，在陆丰13斜坡带发育断穿基底的南倾板式正断层，主要富集于文昌组内；在陆丰13东洼内则发育南倾或北倾正断层，构成似花状组合样式，主要富集于恩平组内（图3b）。陆丰13东洼及陆丰13斜坡带内的三级断裂形成时间存在差异，其中陆丰13斜坡带的板式正断层形成于文昌组沉积期，而洼陷内的似花状正断层组则集中形成于恩平组沉积期。
陆丰15断层（F3）位于凹陷南侧，断层下盘为东沙隆起，是一条近铲式形态的大型北倾正断层（图3c）。断层纵向断穿层位最多，向下断穿至基底，向上终止于万山组内。陆丰15断层在古近纪强烈活动，使陆丰15洼呈南断北超的半地堑结构。生长地层厚度变化表明断层在下文昌组沉积期活动性最强，随后逐渐减弱。三级断裂集中发育于陆丰15斜坡带，以断穿基底的南倾板式或铲式正断层为主，形成于文昌组沉积期，部分断层在恩平组沉积期继续活动，与新形成的断层构成“Y”型组合样式（图3c）。
2.2 平面展布特征
陆丰凹陷南部主要发育NNE、NWW两组基底断裂[23-24]，部分基底断裂在古近纪再活化，走向与基底断裂基本一致，因此断裂在Tg反射层上以NEE、NWW为主（图4a）。在Tg反射层，一级断裂延伸距离远，水平断距大，走向以NWW-EW为主，其中陆丰13东断层的东段为NE走向。三级断裂主要分布于陆丰13东洼和陆丰15洼的斜坡带处，断裂平面延伸短，水平断距小，与一级断裂的走向基本一致。裂陷I幕为NNW向伸展（图2），在凹陷内形成较多三级断裂，T80反射层的断裂优势走向变为NNE向（图4b）。此外，Tg-T80反射层的断裂密集带也由陆丰15斜坡带迁移至陆丰13东断层南部的斜坡带（图4b）。裂陷II幕转为近S-N向伸展（图2），T70反射层的断裂优势走向变为近EW向（图4c）。断裂平面延伸距离较长，但水平断距小，且在该反射层未见明显的断裂密集带，而是在凹陷各处零散分布（图4c）。
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图 4 陆丰凹陷南部不同层位断裂分级展布特征Figure 4. Fault classification and distribution in different horizons in the southern Lufeng Sag3. 断裂活动期次与演化
陆丰凹陷南部地区的断裂主要在古近纪发生活动，但不同断裂的活动期次及强度存在一定差异。断裂生长指数广泛应用于对断裂活动期次及活动强度的判别[25-27]。以位于研究区中部的地震剖面为例进行断裂生长指数分析，其中断层f1-f5在文昌组沉积期活动，生长指数大于1。断层f1、f2和f5断穿基底且在文四段活动强度较大；断层f3的活动强度由下文昌至上文昌组沉积期逐渐增大；断层f6在恩平组沉积期形成并活动。断层F2和f7分别为控洼边层和与之对倾的反向调节断层，在文昌-恩平组沉积期持续活动且活动强度较大（图5）。
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图 5 陆丰凹陷南部典型剖面断层生长指数分析剖面位置见图1b。表格中的红线代表断层断穿的层位，蓝色方块代表生长指数。Figure 5. Analysis of growth index of typical faults in southern Lufeng SagSee section location in Fig.1b. The red line in the table shows the horizon where the fault penetrates through, and the blue square shows the growth index.整体来看，陆丰凹陷南部地区断裂的活动时期与凹陷整体演化阶段基本一致，在裂陷I幕和裂陷II幕均有断裂发生强烈活动。依据断裂活动期次及强度，可将发育于古近纪的断裂划分为3类：文昌期活动断层、恩平期活动断层和文昌-恩平期活动断层。其中文昌期活动断层在文昌组沉积期开始形成并强烈活动，部分向上断穿至恩平组内，但在恩平期一般都活动较弱，属于继承性活动（如f1-f5）。恩平期活动断层可能向下断穿至文昌组内，但在文昌期不活动（如f6）。文昌-恩平期活动断层则是在文昌组和恩平组沉积期均发生强烈活动，控制了洼陷或构造带的结构特征（如f7、F1-F3）。从断裂级别及其活动性来看，一级断层和二级断层主要对应文昌-恩平期活动断层，而三级断层则对应文昌期或恩平期活动断层。
综合区域构造运动及应力场特征，在凹陷构造演化的基础上进一步分析断裂形成演化过程（图6）。受太平洋板块俯冲作用影响，陆丰凹陷南部在裂陷I幕处于NW-SE方向的伸展环境[23-24]，部分NEE、NWW走向基底先存断裂活化，促使文昌期活动断层开始形成，平面走向以NEE和NWW向为主。控洼断层（一级断层）和控带断层（二级断层）在这一时期的活动性逐渐增强，控制各洼陷或构造带的结构特征（图6a-b）。在裂陷II幕，受太平洋板块俯冲后撤和古南海拖曳作用影响，区域伸展方向由NW-SE向转为近S-N向[23-24]，陆丰凹陷发生张扭变形，部分文昌期活动断层发生继承性活动，但活动强度较小。恩平期活动断层在该时期形成，受扭动作用的影响，断层在剖面上呈“Y”型、似花状等组合样式（图6c），在平面上以近E-W走向为主。控洼断层和控带断层在裂陷II幕持续活动，控制洼陷/构造带恩平组的结构特征。
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图 6 陆丰凹陷南部构造演化剖面剖面位置见图1。Figure 6. Tectonic evolution of the southern Lufeng SagSee Fig.1 for section location.后裂陷期分为断拗转换期和拗陷期，断裂逐渐停止活动（图6e-f）。珠海组沉积期，珠江口盆地由陆相变为海相沉积环境，陆丰凹陷南部进入断拗转换阶段。该时期未见新生断层发育，但部分恩平期活动断层可继承性微弱活动（图6e）。拗陷期（珠江组沉积期—现今），陆丰凹陷南部的断裂活动基本停止，极少量断层（如陆丰15断层）在东沙运动时期（韩江组沉积期）发生弱活动（图3c）。拗陷期地层表现为厚层披覆沉积，基本不发生构造变形（图6f）。
4. 断裂对油气成藏控制作用
4.1 断裂与圈闭类型
勘探实践证实，陆丰凹陷南部地区主要发育断鼻、断块和背斜/断背斜等圈闭。断鼻圈闭主要分布在陆丰13东洼和15洼的斜坡带，裂陷I幕控洼断裂强烈活动形成地势斜坡，在砂体上倾方向发育与地层倾向相同的二级和三级断裂，共同组合形成文昌组内的断鼻圈闭。控制断鼻圈闭的三级断裂仅在文昌期活动，活动停止时间较早，在油气成藏期不活动，侧向封闭性较好，油气沿连通砂体运移至圈闭内成藏，如陆丰Z-9构造（图7）。断块圈闭主要分布在陆丰13东洼斜坡带的文昌组内，斜坡带的多条三级断裂在文昌期发生活动，呈多级断阶式组合，断层与地层倾向相反，在断层下盘形成多个小型断块圈闭，油气由生烃洼陷排出后先发生侧向运移，再沿控圈断裂垂向运移至圈闭内。陆丰Z-5构造为断块型圈闭，在斜坡带高部位发育一条规模较大的反向断层，断层侧向封堵性好，油气在该构造圈闭内富集程度高（图7）。断背斜圈闭主要分布在陆丰13东洼和陆丰13西洼的恩平组内，主要为“Y”字形断裂控制的（断）背斜圈闭和位于控洼断裂上盘的滚动背斜圈闭。位于陆丰13东洼的Z-6构造为两条“Y”字型对倾三级断层控制的背斜圈闭，断层在恩平期活动并控制局部构造变形，使断层之间的地层呈背斜形态（图7）。控圈断裂垂向上沟通文四段烃源岩与恩平组圈闭，可为油气垂向运移提供有利通道。陆丰Z-2构造位于陆丰13西断层上盘，裂陷II幕断层强烈活动使上盘地层逆牵引变形，在恩平组内形成滚动背斜圈闭。控洼断裂作为通源断裂且长期活动，有利于油气垂向运移。
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图 7 陆丰凹陷南部断层相关圈闭主要类型Figure 7. Main types of fault-related traps in the southern Lufeng Sag4.2 源-断组合类型与油气运移
断裂可在垂向上沟通烃源岩和圈闭、储层，是油气运移的重要通道[28-30]。陆丰凹陷南部地区的烃源岩以文昌组内的厚层中深湖相烃源岩为主[10, 31]。本文主要从该地区烃源岩形态特征与断裂组合样式角度出发，划分出6类源-断组合类型，包括双向汇聚型、边缘汇聚型、双向发散型、同向输导型、多级断阶型以及反向遮挡型（图8）。
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图 8 陆丰凹陷南部源-断组合类型与油气运移Figure 8. Types of source-fault assemblage and hydrocarbon migration in the southern Lufeng Sag双向汇聚型、边缘汇聚型和双向发散型源-断组合均为通源断裂切穿烃源岩，油气由烃源岩排出后沿断裂垂向运移的模式，主要分布于各洼陷内。这3种类型的主要区别是烃源岩层的形态特征及其与通源断裂之间的匹配关系。双向汇聚型源-断组合的烃源岩层为中部高、两侧低的“汇聚脊”形态，通源断裂切穿烃源岩层中心位置，油气由烃源岩两翼向中央高部位汇聚，再由断裂垂向运移至储层内，油气运聚效率最高，如陆丰Z-6油藏为“Y”字型断裂断穿烃源岩高部位的双向汇聚型源-断组合（图8）。而边缘汇聚型源-断组合的通源断裂未切穿烃源岩中央高部位，在烃源岩内油气仅由单侧向上运移，再经断裂垂向运移至储层，油气运聚效率较低。陆丰Z-7油藏的通源断裂断穿至烃源岩“汇聚脊”的边缘位置，可向储层运移的油气量减少，最终成藏效果较差。陆丰13西洼和陆丰15洼内的烃源岩层为中央下凹、向洼陷边缘发散的状态，属于双向发散型源-断组合，油气由烃源岩向断裂的运移量最少，运聚效率最低，目前在该类型的储层中暂无大规模油气发现（图8）。
同向输导型、多级断阶型及反向遮挡型源-断组合多发育于斜坡带，其中同向输导型和多级断阶型的断裂倾向与烃源岩上倾方向相反，有利于油气沿断裂上盘破碎带垂向运移，但多级断阶型的断裂在油气运移路径上发育较多，在运移时一部分油气可跨越断裂继续侧向运移，但另一部分油气在浮力驱动下沿断裂上盘垂向运移，产生油气分流作用，导致最终可进入目标圈闭的油气量减少，如陆丰Z-3构造等；反向遮挡型源-断组合的断裂倾向与烃源岩上倾方向相同，油气易于在断裂下盘富集成藏，其中陆丰Z-5构造以同向输导型为主，油气运聚效率高，同时在目标圈闭内发育一条反向断层，兼具反向遮挡断层侧向封闭性较好的特性，油气发生大规模聚集（图8）。
4.3 油气成藏组合类型
综合油气富集层系、输导方式、断裂活动性及源-断组合类型等成藏要素，将陆丰凹陷南部的油气成藏组合类型分为源内油气藏和源外油气藏两类，源内油气藏是指油气在烃源岩内的储层或邻近烃源岩的层位内富集成藏，油气未发生大规模运移；源外油气藏是指油气通过断裂、砂体或不整合面在垂向或侧向上长距离运移，在距离烃源岩较远的储层内富集成藏。其中，源内油气藏可进一步细分为自生自储型、自生上储型源内油气成藏组合两个亚类；源外油气藏可细分为旁生侧储型、下生上储型源外油气成藏组合两个亚类（图9）。
源内油气藏的油气主要富集于下部文昌组内，文昌组各段地层均发育规模不等的中深湖、滨浅湖相烃源岩，油气自文昌组烃源岩排出后近距离运移。自生自储型组合的油藏常见于陆丰13斜坡带，物源区碎屑物质在文昌组沉积期入湖，在斜坡带沉积辫状河三角洲连通砂体，提供侧向运移通道；油气自文四段烃源岩排出后，可直接进入下文昌组的连通砂体侧向运移，在储层圈闭内聚集成藏，一般为岩性油藏或断裂-岩性复合油藏。而下生上储型油气成藏组合有断裂参与油气运移过程，或早期自生自储型组合类型的油藏受后期断裂调整，油气运移至上文昌组内成藏，主要为断块、断鼻等构造油藏类型。这两类油气成藏组合类型的主要区别在于断裂是否直接参与油气运移过程。陆丰Z-5、Z-4、Z-9构造均为典型的源内油藏组合类型（图9）。
源外油气藏的油气主要富集于上部恩平组内，油气自文昌组烃源岩排出后发生长距离运移，且需通过断裂进行垂向运移。旁生侧储型组合的油气藏位于斜坡带高部位，油藏埋深浅，多为垂向多层叠置，在平面上成片分布。油气自文昌组烃源岩排出后先沿砂体连通孔隙或不整合面侧向运移，再经断裂垂向运移至储层内成藏，主要为断块、断鼻或断背斜等构造油藏。下生上储型组合的油气藏主要位于陆丰13东洼、西洼内，恩平组储层位于洼陷内的主力烃源岩正上方，通源断裂沟通深层烃源岩与浅层储层圈闭，油气自烃源岩排出后由断层垂向运移，在恩平组内富集成藏，多为断块或背斜类构造油藏。此类油藏也具有单油层厚度小、数量多的特点，但同一构造带内的各油层总资源量大。陆丰Z-6、Z-2等构造为典型源外油藏类型（图9）。
5. 结论
（1）陆丰凹陷南部地区主要发育3个半地堑式洼陷，古近系断裂在斜坡带密集发育，断裂多为单期活动，平面上断裂优势走向由深层NEE向至浅层近SN向偏转，断裂密集带由东向西迁移。
（2）断裂主要在文昌期、恩平期和文昌-恩平期发生活动，并控制了断鼻、断块和断背斜圈闭的形成，其中断鼻、断块圈闭主要受控于二级和三级断裂，而断背斜圈闭主要受控于一级和二级断裂。断裂与烃源岩的组合型式影响了油气运聚效率，其中双向汇聚型、同向输导型和反向遮挡型源-断组合的油气运聚效率较高。
（3）陆丰凹陷南部主要发育源内自生自储型组合、源内自生上储型组合、源外旁生侧储型组合、源外下生上储型组合4类油气成藏组合类型。源内成藏组合类型主要为岩性油藏、构造油藏和少量构造-岩性复合油藏，源外成藏组合类型主要为构造油藏。
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图 1 南黄海辐射沙脊群西洋潮流通道及其邻区遥感影像
Figure 1. Remote sensing imageries of the Xiyang tidal channel in the Radial Sand Ridge Field, South Yellow Sea and its adjacent regions
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图 2 前人对西洋潮流通道浅部沉积层序和年代框架的三类观点及本文研究再认识的第四类观点
Figure 2. Previous three viewpoints on the sedimentary sequence and chronology framework of the Xiyang tidal channel in the Radial Sand Ridge Field and the fourth viewpoint derived from the restudy of this paper
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图 3 辐射沙脊群西洋潮流通道的浅层地震剖面测线和钻孔位置
注：因西洋及周边区域缺乏最新完整的水深实测资料，故图3的底图水深取自1979年海图，加之辐射沙脊群局部区域动力地貌调整明显，因而此图上西洋周边潮滩和沙脊形态与近期遥感影像存在一定差异。
Figure 3. Location of shallow seismic profiles and sedimentary cores in the Xiyang tidal channel, Radial Sand Ridge Filed
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图 4 西洋潮流通道SD1307F1-1测线浅层地震剖面及其解译
图中U为地震单元，T为反射界面。
Figure 4. Shallow seismic profile SD1307F1-1 in the Xiyang tidal channel and its interpretation
U: seismic unit, T: seismic bounding surface.
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图 5 西洋潮流通道SD11-01-04测线浅层地震剖面及其解译
图中U为地震单元，T为反射界面。
Figure 5. Shallow seismic profile SD11-01-04 in the Xiyang tidal channel and its interpretation
U: seismic unit, T: seismic bounding surface.
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图 6 西洋潮流通道东南段07SR01孔与G39孔、Y1孔沉积层序对比
07SR01孔据文献[50-51]改绘，G39孔据文献[61]改绘，Y1孔据文献[53,62]改绘，海面变化曲线据文献[11]改绘。
Figure 6. Stratigraphic correlation among core 07SR01, G39 and Y1 in the southeastern part of Xiyang tidal channel
Core 07SR01 was modified after reference [50-51], Core G39 was modified after reference [61], Core Y1 was modified after reference [53,62], Curve of sea-level changes was modified after reference [11].
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图 7 大丰港西北侧DFA08孔揭露的典型第二陆相沉积层及其沉积环境解释
岩心照片由江苏省有色金属华东地质勘查局提供，图上右侧数值为岩心段埋深值。
Figure 7. A typical second continental sedimentary layer revealed by core DFA08 in the northwest of Dafeng Port and its interpretation of sedimentary environments
The core photo was provided by East China Geological Exploration Bureau of Nonferrous Metals, Jiangsu Province. The value on the right of the figure is the buried depth of the core section.
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图 8 进一步研究西洋潮流通道浅部沉积层序及其形成演化的技术路线
Figure 8. Technical route of further study on the shallow sedimentary sequence and its evolution of the Xiyang tidal channel
表 1 西洋潮流通道周围第一陆相层底部和上覆沉积的14C测年数据
Table 1 14C dating ages of the bottom and overlying deposits of the first continental layer around the Xiyang tidal channel
钻孔编号 地理位置 埋深/m 测年材料 14C年龄
/aBP数据来源 PY19 东台新曹 33 泥炭 36470±2000 文献[65] DF02 大丰港区陆域 20.5 软体动物壳 7040±30 文献[69] SC 东台三仓 8 软体动物壳 670±30 文献[74] 21.5 软体动物壳 5890±180 文献[75] JC-1204 东台三仓 10.86 软体动物壳 1090±30 文献[71] 14.09 软体动物壳 4040±30 YZ08 东台弶港 7.38 软体动物壳 640±30 文献[70] 8.28 软体动物壳 690±30 10.68 软体动物壳 770±30 14.18 软体动物壳 830±30 19.22 软体动物壳 1140±30 19.73 软体动物壳 1070±30 20.22 软体动物壳 1000±30 22.64 炭屑 3870±30 25.41 软体动物壳 5300±30 29.42 软体动物壳 8360±30 Y5 高泥
（西洋南侧）3.08 软体动物壳 520±30 文献[53] 5.85 植物碎屑 560±30 10.12 软体动物壳 690±30 15.24 软体动物壳 790±30 17.26 软体动物壳 880±30 19.48 软体动物壳 6180±30 
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