Holocene extreme flood events in the Yangtze River Basin: Research progress and implications
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摘要:
随着全球气候变暖和人类活动加剧，全球洪水事件的发生频率与强度正在快速变化，揭示洪水发生规律及其驱动机制是当前古洪水水文学和全球变化研究的热点问题。长江流域作为中国洪涝灾害最为严重的区域之一，其洪水活动近年来呈现快速异常变化，较短的现代器测记录已不能满足未来洪水灾害风险预测的需求，迫切需要通过各种长时间尺度记录揭示过去时期长江流域洪水事件与气候变化之间的关系。本文通过综述各种极端洪水事件的地质记录和历史记录，确定全新世以来极端洪水事件的频发期，并与区域关键气候代用指标进行对比，发现洪水事件频发期主要跟气候的急剧突变和强烈的人类活动有关。然而准确预测长江流域洪水事件未来演化趋势，需不断加强各种代用记录的综合研究，进一步探索洪水发生机制与气候变化和人类活动耦合关系，并加强有关数值模拟方面的研究，以便于为未来长江流域的洪涝灾害防御、城乡规划优化布局、资源合理开发利用提供科学依据和决策支持。
Abstract:With global warming and the intensification of human activities, the frequency and magnitude of large river flood events are increasing in recent years. To reveal the regularity of flood occurrence and its driving mechanism is a hot issue in the study of paleoflood hydrology and global change. As one of the regions with the most severe flood disasters in China, the Yangtze River Basin has shown rapid and abnormal changes in flood activities in recent years. Short modern measurement records can no longer meet the needs of future flood disaster risk prediction, and it is urgent to reveal the relationship between flood events and climate change in the Yangtze River Basin in the past through various long-term records. By summarizing the geological and historical records of various extreme flood events, the frequent periods of extreme flood events since the Holocene were determined and compared with key regional climate proxies. However, to accurately predict the future evolution trend of flood events in the Yangtze River Basin, it is necessary to strengthen continuously the comprehensive research of various proxy records, to further explore the coupling relationship of flood occurrence mechanisms to climate changes and human activities, and to strengthen research on numerical simulation. This study provided a scientific basis and decision support for future flood disaster prevention, urban and rural planning optimization layout, and rational resource development and utilization in the Yangtze River Basin.
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Keywords:
- paleoflood events /
- sedimentary record /
- global warming /
- human activities /
- the Yangtze River
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平北地区面积近1 800 km2（图1），自1988年钻探宝云亭1井以来，经过30年的勘探开发，已建成投产3个油气田，主要勘探目的层为中上始新统平湖组。勘探初期由于缺少三维地震资料，多利用二维地震测线开展工作，主要以勘探构造油气藏为主，预探井多布署在构造高点。随着三维地震资料覆盖率的增加，勘探及开发工作的不断深入，发现部分已钻的构造圈闭不落实，圈闭无效，钻遇的气藏为构造―岩性复合气藏；同时3个气田的多口开发井也证实，砂体在平面上连续性差，气藏多受构造和岩性双重因素控制，因此，平北地区构造―岩性复合圈闭具有较大的勘探潜力。平北地区剩余构造圈闭数量少，条件差，资源规模小，可钻探性低，截止目前，平北地区探井密度约为0.017口/km2，勘探程度低，勘探潜力大，因此，构造―岩性复合圈闭、岩性圈闭应为下一步的主要勘探方向。
对于断陷期构造―岩性复合圈闭的勘探而言，砂体的展布范围不仅控制了圈闭规模的大小，更从根本上决定了圈闭是否存在，因此，弄清砂体的展布形态至关重要。前人研究表明，砂体的分布及富集受多重地质因素的控制。贾承造等认为盆地的构造运动、古气候变迁、古物源等因素控制了砂体形成和分布[1]；李丕龙等认为陆相断陷盆地不同断裂形成的断阶、段坡或断裂坡折带等对砂体发育与分布起着重要的控制作用[2]；邹才能等提出陆相断陷盆地内砂体分布主要受控于斜坡、断裂和水深3个重要因素[3]；冯有良提出层序界面控制了地层油气藏的发育，盆缘的沟谷和构造坡折带控制的层序低位体系域和高位体系域砂体是岩性油气藏的主要储集体[4]。赵贤正等以二连盆地为例，认为砂体的展布主要受到构造带类型、同沉积断层组合样式、体系域类型、坡折带类型及沉积相类型的控制[5-6]。
通过对西湖凹陷保俶斜坡带平北地区砂体的形成和分布的研究认为该区为缓坡背景，砂体分布主要受到构造古地貌、坡折带类型、层序样式及沉积微相类型的控制。
1. 构造古地貌及可容纳空间控制地层厚度及沉积体规模
西湖凹陷自西向东可以划分为保俶斜坡带、三潭深凹带、中央背斜带、白堤深凹带及天屏断阶带5个次级构造单元。平北地区位于保俶斜坡带中段，总体上呈西南高、北东低的斜坡。主力勘探目的层中上始新统平湖组为一个从水进到水退的过程[7]，从下至上可划分为平下段、平中段及平上段3个段，平下段可进一步划分为平下下、平下上2个亚段。
平湖组早期继承了基底先存古地貌，自南向北发育宝云亭、武云亭、孔雀亭3个古鼻隆，具有隆洼相间的地貌格局，西部海礁凸起长期遭受剥蚀，为主要物源区，沉积物通过古地貌沟谷、断槽物源通道大量卸载于具有较大可容纳空间的古地貌低洼区，造成古隆起上下地层厚度差别大，在古地貌低洼区可达800 m以上，斜坡大部分地区为200～300 m（图2）。同时，受古地貌限制，沉积体及砂体展布范围较局限。
![图 2 平湖组不同时期古地貌图、地层厚度图、沉积体展布范围对比图]()
图 2 平湖组不同时期古地貌图、地层厚度图、沉积体展布范围对比图Figure 2. Diagram of paleogeomorphy, strata thickness and depositional areas in different stages of Pinghu Formation平下上段，构造活动及古地貌分隔性有所减弱，但该时期古地貌依然是沉积体发育的主要控制因素，地层厚度为0～600 m，沉积物仍主要卸载于古地貌低势区（图2）。同时，该期为平湖组最大海泛期，A/S比较高，整体上沉积体及砂体规模较小，但也不乏局部古地貌低洼处较厚砂体富集。例如C5井，在平下段单层厚度＞30 m，累计储层厚度＞70 m的砂层。
平中段进入断拗转换阶段，构造活动大幅减弱，随着海进到海退的转换，整个斜坡以填平补齐作用为主，地层展布范围大，厚度更加均衡，沉积体规模增大（图2），以向海方向进积的三角洲为主，砂体分布范围更大，连续性更好。
平上段平北地区形成一个宽缓的斜坡，构造古地貌对沉积体控制作用基本消失，沉积类型以规模较平中段更大的三角洲为主，地层厚度为0～300 m，厚度差进一步减小（图2），砂体更加发育，连续性增强。
2. 同沉积断裂坡折带控制砂体的展布
长期活动的同沉积断裂形成的“构造坡折带”制约着盆地充填可容纳空间的变化，控制着低水位体系域、高水位体系域三角洲―岸线体系的发育部位，对沉积体系的发育和砂体分布起重要的控制作用[8-10]。平湖组沉积于中―晚始新世断陷―断拗转换期，断裂活动对砂体的发育展布具有较强的控制作用，尤其是断层活动较强的平下下段及平下上段。
平北地区发育二级―五级断裂，其中三级及以上断裂组成的断裂坡折带对沉积及砂体具有明显的控制作用。在始新世持续性北西―南东方向扭张力作用下形成一系列NE―SW走向的断裂体系（图3）。同时，受控于先存古地貌，平北地区自南向北发育4种断裂系统组合样式。
![图 3 平北地区断裂体系、组合方式及控砂模式图]()
图 3 平北地区断裂体系、组合方式及控砂模式图Figure 3. Map of fractures system and their distribution patterns and their control over sandbodies in Pingbei region2.1 帚状断阶断裂坡折带及砂体分布样式
帚状断裂坡折带见于A区，以发育一条控凹的二级边界主断裂为特征，垂向断距最大可达4 000 m，主断裂北部末端呈帚状撒开，分枝成若干条三级―四级次级伴生断裂，其中三级断裂的平面延伸长度约10 km，垂向断距约1 000 m，对沉积及砂体的展布具有较强的控制作用。四级断裂垂向断距约500 m，对砂体的控制作用较小。这种断裂的形成一般与凹陷走滑作用有关。帚状断裂坡折带对沉积体及砂体的控制作用主要表现为主干断裂捕获其上升盘水系，控制碎屑体系向凹陷内的推进方向，主干断裂的延伸方向及发散部位控制着沉积中心及砂体分布。在主干断裂主体部位下降盘或内叉角的构造低部位砂体厚度较大，形成“断角砂体”。该区位于主干断裂下降盘的A3井平下段均发育厚层砂体。而帚状末端四级断裂控制的A5井砂体则欠发育（图3）。
2.2 垒堑组合断裂坡折带及砂体分布样式
垒堑组合型断裂坡折带发育于B区、C区。这种断裂坡折带的主要特征为发育2组相对倾向的断裂，平面上与斜坡倾向相同的顺向断裂（B区）呈平行式展布，多为三级断裂，与斜坡倾向相反的反向断裂（C区）多为反“y”字型组合，垂向上形成多个反向翘倾的半地堑构造。这种断裂坡折带组合的发育与宝云亭古隆鼻的有关。垒堑相间型断裂坡折带对沉积及砂体的控制作用主要体现在反向大断裂捕获其上游的沉积体，使沉积物沿限定型地堑的大断裂根部向前推进，垂直于断裂，沿翘倾方向砂体逐渐减薄尖灭。每个三级反向断裂控制一个半地堑，形成一个沉积中心（图3）。C5井靠近反向断裂根部，平下段发育多层厚层砂体，向翘倾方向C4井砂体逐渐减薄，而位于翘倾端的C3井砂体已尖灭，发育泥岩。而地垒上砂体整体发育欠佳，较厚层的砂体主要发育于古隆起上的次级低洼区。
2.3 顺向翘倾断块断裂坡折带及砂体分布样式
顺向翘倾断块型断裂坡折带主要发育于D区，以伸展构造样式为主。平面上2～3条NE―SW走向的三级弧形断裂形成一个控沉积坡折带，由斜坡高部位到低部位发育4个断裂坡折带，垂向上由坡折带形成逐级下掉的顺向翘倾断块。顺向翘倾断块断裂坡折带对沉积的控制作用一方面体现在两条断层相交处容易形成沉积物输送通道，另一方面，沉积体垂直于断层走向上沿断阶逐级沉积，由于翘倾作用，断层根部具有相对较大的可容空间，形成较厚砂体堆积（图3）。D区的8口钻井均钻探在靠近断层根部处，均在平下段钻遇较厚砂体。
3. 体系域类型控制砂体的时空配置
据经典层序地层学原理，可将一套完整的层序运用三分法划分出低位体系域、海侵体系域和高位体系域。体系域的形成与可容空间变化有着十分密切的联系，随着可容空间的变化，不同类型体系域控制了各沉积体系砂体的形成与分布[11-15]。西湖凹陷始新统平湖组为一个完整的二级层序。在二级层序格架内划分了低位体系域平下下段，海侵体系域平下上段及高位体系域平中―上段。
3.1 低位体系域（LST）
低位体系域（LST）期，基准面上升缓慢，沉积物供给速率大于可容空间增加速率，通常情况下以发育富砂质的扇三角洲、辫状河三角洲沉积。平北地区低位体系域发育时期受到强烈的断陷作用及古地貌格局的限制，发育近物源，限定型的潮控三角洲沉积（图2）。钻井揭示平下下段的厚层砂岩发育，多为中粗砂岩，常含砾，测井曲线多呈箱型，具有正旋回。砂地比为30%～50%（图5），研究认为：当地层砂地比＞60%，发育构造圈闭，砂地比＜30%发育岩性圈闭，介于两者中间的多发育构造―岩性复合圈闭[6]。因此，就沉积序列而言，平下段适合构造―岩性复合圈闭的发育，同时，其上覆的平下上段大规模海侵泥岩也具备形成区域性盖层的条件，具备很好的储盖组合匹配条件（图4，图5）。而目前，平北地区平下下多口钻井均揭示构造―岩性复合圈闭，直接证明平下下段具备发育复合圈闭的地质条件。
![图 5 平北地区典型钻井层序对比图]()
图 5 平北地区典型钻井层序对比图Figure 5. Sequence stratigraphic profile of typical wells in Pingbei region![图 4 平北地区层序模式图（以垒堑型为例）]()
图 4 平北地区层序模式图（以垒堑型为例）Figure 4. Sequence stratigraphy of the Pingbei region（Take the horst-graben pattern for example）3.2 海侵体系域（TST）
海侵体系域（TST），基准面快速上升，沉积物供给速率远小于新增可容空间速率，通常易形成退积型近岸水下扇砂体。平北地区海侵体系域发育时期，断陷作用逐渐趋弱，但海平面快速的上升仍然使可容空间增加速率远大于沉积物供给速率。沉积体快速向陆方向退积，虽然仍发育受古地貌限定型的辫状河三角洲沉积，但沉积体规模缩小。钻井揭示平下上段地层具有“泥包砂”的特征，大多数钻井泥地比在70%以上，是一套泥岩厚度大，横向分布稳定，具有一定可对比性的区域性盖层（图4）。只在局部断层“聚砂”作用强烈处见具有一定厚度的砂岩发育。这种沉积建造对于岩性圈闭的发育提供很好的条件，孤立的砂岩被泥岩包裹，具有很好的生排烃条件及封堵条件。同时由于泥岩生烃等作用容易在砂岩中形成高压，对储层物性起到较好的保护作用。C区的C5井在平下上段钻遇的这类气藏物性好，产量高（图4）。
3.3 高位体系域（HST）
在高水位时期，受气候、构造及外部水系等因素影响基准面呈高频率的变化，沉积物供给速率等于或大于新增可容空间速率，通常发育加积型或进积型扇三角洲砂体。平中―上段西湖凹陷进入断拗转换阶段，构造趋于稳定，平北地区发育填平补齐的沉积作用，发育规模较大的受潮汐影响三角洲沉积。钻井揭示平上段砂体层数多，厚度大，砂地比最高可达80%，砂体横向连续性变好（图5）。在较高的砂地比条件下，不利于岩性圈闭的形成，侧向需要依靠断层形成封堵。同时，平湖组高位体系域上覆为渐新统花港组低位域富砂沉积，缺乏区域性泥岩盖层，不利于油气藏的保存，对于岩性圈闭的勘探应主要关注三角洲前缘砂地比降低至60%以下的地区。
4. 沉积相带控制砂体的储层物性
盆地的构造、沉积背景决定其沉积体系的形成和展布，不同类型沉积相对砂体的储集特征具有重要的控制作用，不同类型砂体的沉积构造、沉积韵律、厚度、岩性储集特征都存在着差异[16]。西湖凹陷平湖组具有局限海湾的沉积背景，发育辫状河三角洲―潮坪共生沉积体系。
平下下及平下上段，断陷作用形成较大的可容空间，在河流及轴向潮流的作用下发育潮控三角洲及河口湾沉积，河口湾前端发育放射状湾口型砂脊（图6）。砂体类型有三角洲前缘分流河道砂、潮道砂、潮坪砂、河口湾砂坝砂及潮汐砂脊砂。在潮汐能量较强的水动力环境下，三角洲前缘水下分流河道与潮道常具有相似的岩电特征，难以区分，统称为水道。目前，平北地区钻井已证实具有良好储集性能的砂体类型有：水道砂及河口湾砂坝砂。水道砂单层厚度一般为20～70 m，岩性以浅灰色中―粗砂岩为主，底部多含砾，测井曲线多呈微齿化箱型或钟型，岩心多见强水动力作用形成的板状交错层理、底砾及侵蚀面等（表1）。在埋深4 000 m以下仍保留部分原生孔隙，平均孔隙度为12.5%，平均渗透率可达5 mD。是平北地区深层优质的储层。河口湾砂坝主要发育在平北北部地区，钻井上单层厚度为10～30 m，以浅灰色细―粗砂岩为主（表1），偶含砾，测井曲线呈微齿化箱型或钟型，岩心上以较强水流形成的板状和平行层理为主。这类砂体由于受到潮汐水流的反复淘洗，成熟度高，抗压实能力强，在埋深大于4 100 m时仍保留部分原生孔隙，并常见溶孔和铸模孔。孔隙度为10%～20%，渗透率约为0.49～145 mD，平面上具有较强的非均质性。
表 1 平北地区不同类型砂体特征Table 1. The characteristics of different sandbodies in Pingbei region砂体类型 平下段 平中-上段 水道 河口湾砂坝 水下分流河道 单砂厚 20～70m 10～30m 10～40m 颜色 浅灰、灰白 浅灰、灰白 浅灰、灰白 岩性 砂岩 砂岩 砂岩 粒度 中-粗砂，含砾 细-粗砂，偶含砾 细砂-砾岩 岩电特征 
沉积构造 
孔隙度（%） 9.9～15（12.5） 9～19.56（13.77） 8～22.23（13.12） 渗透率（mD） 0.5～31.6（5.1） 0.49～145（21.88） 1～227（35.98） 平中―上段斜坡区构造稳定，断层活动微弱或停止活动，填平补齐及持续性海退，海湾内主要以平行岸线的潮流作用为主，沉积体以规模逐渐增大的受潮汐影响的非对称三角洲为主，三角洲逐渐向凹陷中央推进，三角洲前端发育受潮汐改造形成的与岸线斜交的潮汐砂脊（图7）。储集条件较好的砂体类型主要有三角洲前缘水下分流河道砂、潮汐砂脊砂。钻井揭示的三角洲前缘水下分流河道砂岩厚度多为30 m，岩性以浅灰色细砂岩―砾岩为主，测井曲线呈微齿化箱型，岩心上可见圆―次圆状的砾石定向排列及板状交错层理等反应牵引流沉积构造（表1）。水下分流河道砂岩在4 200 m埋深下仍保持部分原生孔隙，孔隙度多在10%以上，渗透率多大于1 mD，为平中上段有利储层。同时，砂脊砂目前虽未有钻井揭示，但从成因上，潮汐砂脊是三角洲前缘砂体经过潮汐等较强水流改造形成的，砂岩通常具有厚度大，成熟度高，抗压实能力强的特征，推测应具有较好的储层物性。并且潮汐砂脊常成群成带分布，易形成叠合连片的规模储量，是优质的勘探目标。
5. 结论
（1）平北地区砂体的发育及展布受古地貌及可容纳空间、同沉积断裂破折带、体系域类型以及沉积相类型多重因素控制。
（2）古地貌及可容纳空间从宏观上控制了地层厚度及沉积体规模，在此基础上由同沉积断裂坡折带及体系域类型具体控制了砂体的展布和时空配置关系，而沉积相类型控制了砂体的储集物性。
（3）平北地区平湖组平下下及平下上段是构造―岩性圈闭发育的主要层段，勘探方向为低位体系域控沉积断层下降盘的地势低洼汇砂区，而平中上段砂岩相对更发育，有利的岩性圈闭勘探区为三角洲前缘砂地比低或三角洲前端发育的潮汐砂脊带。
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图 1 长江流域极端洪水记录研究点分布
Figure 1. Study sites of extreme events in the Yangtze River Basin
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图 2 古洪水滞流沉积物野外位置及重建洪水方法
a：古洪水滞流沉积物示意图[65]，b： 三种确定洪水水位方法示意图[66]（据文献[65-66]修改）。
Figure 2. Field location of paleoflood sediment and flood reconstruction method
a: The schematic diagram of paleoflood SWD[65],b: Schematic diagram of three methods for determining flood level[66] (Modified according to references [65-66]).
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图 7 长江流域全新世洪水记录及其与气候和人类活动记录的对比
a: 和尚洞石笋HS4的IRMsoft-flux[101], b: 10 000 cal. aBP以来北半球夏季太阳辐射变化[120]， c: Huang等重建的10 000以来气温变化[121]，d: 10 000 cal. aBP以来El Junco粉砂记录的ENSO变化情况[122]， e: 阿曼Qunf洞穴石笋所记录的δ18O数据指示西南季风变化[123]， f: 湖北神农架地区三宝洞石笋所记录的δ18O指示东亚季风变化[124]， g: HYDE3.0数据库10 000 cal. aBP以来江汉平原地区人口密度变化[125]， h: HYDE3.0数据库10 000 cal. aBP以来江汉平原地区耕地垦殖率变化[125]（图中6处阴影从左至右分别对应LIA-小冰期、MCA-中世纪气候异常、DACP-黑暗时代冷期、RWP-罗马暖期、4.2ka寒冷事件、8.2ka寒冷事件）。
Figure 7. The Holocene flood records in the Yangtze River Basin and their comparison with climatic and human activity records
a: IRMsoft-flux in stalagmite HS4, Heshang Cave[101], b: changes of solar radiation in the northern hemisphere during summer since 10000 cal.aBP[120], c: changes in temperature over the past 10,000 years as reconstructed by Huang et al.[121], d: changes of ENSO recorded in El Junco silt since 10000 cal. aBP[122], e: the δ18O data recorded by stalagmites in Qunf Cave, Oman, indicate changes in the southwest monsoon[123], f: the δ18O recorded by stalagmites in Sanbao Cave, Shennongjia area, Hubei Province indicates the change of East Asian monsoon[124],g: the change of population density in Jianghan Plain area since 10000 cal. aBP is obtained by HYDE3.0 database [125] ,h: changes of cropland cultivation ratio in Jianghan Plain since 10000 cal. aBP[125] (The six shadows in the figure correspond from left to right to LIA- Little Ice Age, MCA-Medieval Climate Anomaly, DACP-Dark Age Cold Period, RWP-Roman Warm Period, 4.2ka cold event, and 8.2ka cold event respectively).
表 1 长江流域极端洪水事件研究剖面位置及代用指标
Table 1 Site and proxy of research profiles of extreme flood events in Yangtze River Basin
序号 河段 剖面位置 经纬度 地质记录类型 文献来源 1 上游 中坝遗址 30.34°N、108.45°E 文化遗址 [12] 2 玉溪遗址 30.03°N、107.86°E 文化遗址 [13] 3 红桥村 30.68°N、103.88°E 文化遗址 [14] 4 金沙遗址 30.68°N、104.00°E 文化遗址 [15] 5 马街遗址 30.89°N、103.92°E 文化遗址 [16] 6 张家湾遗址 31.27°N、109.77°E 文化遗址 [17] 7 汉东城遗址 29.00°N、105.84°E 文化遗址 [18] 8 涪碛口遗址 29.20°N、108.75°E 文化遗址 [19] 9 中游 曲远河 32.87°N、110.62°E 自然剖面 [20] 10 尚家河 32.84°N、110.46°E 自然剖面 [21] 11 庹家洲 32.85°N、110.39°E 自然剖面 [22] 12 庹家湾 32.86°N、110.39°E 自然剖面 [23] 13 李家咀 32.82°N、110.77°E 自然剖面 [24] 14 晏家棚 32.83°N、110.43°E 自然剖面 [25] 15 归仙河口 32.82°N、110.54°E 自然剖面 [22] 16 弥陀寺 32.82°N、110.58°E 自然剖面 [26] 17 前坊村 32.83°N、110.98°E 自然剖面 [27] 18 辽瓦店 32.82°N、110.68°E 自然剖面 [24] 19 黄坪村 32.84°N、110.74°E 自然剖面 [28] 20 万春村 33.19°N、107.69°E 自然剖面 [29] 21 祥龙洞 33.00°N、106.33°E 自然剖面 [30] 22 尾笔村 30.39°N、114.47°E 自然剖面 [31] 23 焦家台子 32.82°N、110.16°E 自然剖面 [32] 24 罗家滩 32.78°N、109.35°E 自然剖面 [33] 25 楼子滩 33.46°N、110.51°E 自然剖面 [34] 26 泥沟口 32.89°N、109.53°E 自然剖面 [35] 27 立石村 30.20°N、105.30°E 自然剖面 [36] 28 新滩村 32.76°N、109.33°E 自然剖面 [37] 29 杜家沟 33.19°N、107.67°E 自然剖面 [38] 30 三房湾 30.46°N、113.04°E 自然剖面 [39] 31 江北农场二砖厂 30.18°N、112.34°E 自然剖面 [40] 32 消泗剖面 30.32°N、113.78°E 自然剖面 [41] 33 武汉 30.64°N、114.34°E 自然剖面 [42] 34 SK10 30.60°N、114.31°E 自然剖面 [43] 35 ZK145 30.66°N、114.44°E 自然剖面 [44-45] 36 钟桥遗址 30.31°N、112.27°E 文化遗址 [46] 37 中游 JH001 30.52°N、114.39°E 自然剖面 [47] 38 扬子江剖面 30.30°N、112.12°E 自然剖面 [48] 39 网湖 29.86°N、115.33°E 自然剖面 [49] 40 中洲子 29.80°N、112.75°E 自然剖面 [50] 41 天鹅洲 29.85°N、112.57°E 自然剖面 [51] 42 下游 修河 29.05°N、115.83°E 自然剖面 [52] 43 赣江 29.10°N、116.00°E 自然剖面 [52] 44 黄茅潭 29.80°N、116.35°E 自然剖面 [52] 45 大汊湖 29.10°N、116.01°E 自然剖面 [52] 46 东门镇林峰桥 32.14°N、118.70°E 自然剖面 [53] 47 宝华山-和平冲 32.16°N、119.02°E 自然剖面 [54] 48 宝华山 32.13°N、119.09°E 自然剖面 [54] 
下载: 导出CSV
表 2 长江流域滞流沉积物与冲积平原沉积物宏观特征对比
Table 2 Comparison of macroscopic characteristics of slack water deposits in the Yangtze River Basin and overbank flooding deposits in the floodplain
下载: 导出CSV
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