岩性油气藏 ›› 2026, Vol. 38 ›› Issue (1): 38–54.doi: 10.12108/yxyqc.20260104

• 地质勘探 • 上一篇    下一篇

湖相碎屑岩高频层序地层新认识：来自古代沉积层序的启示

ZAVALA Carlos1, 刘化清2,3, 李相博2,3(), 杨占龙2,3, 李阳1,4,5, 王菁2,3, TROBBIANI Valentin6,7, ARCURI Mariano6,7   

  1. 1 山东科技大学 地球科学与工程学院， 山东 青岛 266590
    2 中国石油勘探开发研究院 西北分院， 兰州 730020
    3 中国石油集团油藏描述重点实验室， 兰州 730020
    4 北京大学 能源研究院， 北京 100871
    5 内蒙古自治区深层煤层气成藏机制与高效开发重点实验室， 内蒙古 鄂尔多斯 017010
    6 阿根廷国立南方大学 地质学系， 布兰卡港 8000
    7 阿根廷GCS公司， 布兰卡港 8000
  • 收稿日期:2025-08-11 修回日期:2025-09-11 出版日期:2026-01-01 发布日期:2026-01-23
  • 通信作者: 李相博
  • 基金资助:
    新型油气勘探开发国家科技重大专项“鄂尔多斯盆地三叠系陆相页岩油勘探开发技术与集成示范”(2025ZD1404800);与国家自然科学基金项目“鄂尔多斯盆地延长组深水块状砂岩形成机理及沉积模式研究”(41772099)

Progress in high-frequency sequence stratigraphy of clastic lakes: Implications from ancient sedimentary sequences

ZAVALA Carlos1, LIU Huaqing2,3, LI Xiangbo2,3(), YANG Zhanlong2,3, LI Yang1,4,5, WANG Jing2,3, TROBBIANI Valentin6,7, ARCURI Mariano6,7   

  1. 1 College of Earth Science and Engineering, Shandong University of Science and Technology, Qingdao 266590, Shandong, China
    2 PetroChina Research Institute of Petroleum Exploration and Development-Northwest, Lanzhou 730020, China
    3 Key Laboratory of Petroleum Reservoir Description, CNPC, Lanzhou 730020, China
    4 Institute of Energy, Peking University, Beijing 100871, China
    5 Inner Mongolia Key Laboratory of Deep Coalbed Methane Accumulation Mechanism and Efficient Development, Ordos 017010, Inner Mongolia, China
    6 Departamento de Geología, Universidad Nacional del Sur (UNS), Bahia Blanca 8000, Argentina
    7 GCS Consulting Services, Bahia Blanca 8000, Argentina
  • Received:2025-08-11 Revised:2025-09-11 Online:2026-01-01 Published:2026-01-23
  • Contact: LI Xiangbo E-mail:lixiangbo911@sina.com

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摘要：

层序地层学理论和方法为地层分析提供了新工具，有助于深化对沉积模式和盆地演化的理解。传统的层序地层学理论中，沉积单元与部分名词术语（如层序界面、体系域、准层序等）是主要针对海相沉积系统提出的，而湖相沉积系统因受构造运动与高频气候旋回的复合控制，非海平面变化驱动，其层序地层特征的复杂程度远高于海相沉积系统。通过对不同湖盆类型的沉积体系的系统解剖，厘清了湖相沉积层序地层学的相关概念，并探讨了他旋回对湖相沉积和层序地层的控制作用以及湖盆可容纳空间类型及其对层序地层和油气成因的意义。研究结果表明：①湖泊沉积状态可划分为3种类型，即欠填充、平衡填充和过填充湖泊，不同状态下湖泊的水体盐度、沉积层序、体系域等具有显著差别。在欠填充时期，湖泊水体是完全封闭的，受高频干湿气候循环影响，湖平面波动变化较大，在潮湿期，河流可提供大量水和沉积物，湖平面上升形成湖侵域（TST），发育向上变细变薄的沉积层序单元（EDS）；在干旱期，湖平面下降，湖盆边缘区域暴露，形成湖退域（RST），湖水盐度为微咸水—超咸水。在平衡填充时期，湖泊呈半封闭状态，兼具欠填充和过填充双重特征，在TST发育期，湖泊呈欠填充状态，随着河流水和沉积物的持续供给，形成向上变细的沉积层序，直到湖平面达到最大洪泛期的溢出点；在RST发育期，湖泊呈过填充状态，发育向上变粗的前积型滨岸三角洲和水下三角洲沉积，此时湖水盐度为咸水—淡水。在过填充时期，湖泊的水体环境是开放的，即湖平面始终维持在湖泊溢出点附近，注入的多余河水会通过溢出点流出，其沉积物主要形成于RST期，表现为向上变粗的前积型滨岸沉积及水下三角洲沉积，且大多数过填充湖泊为淡水湖。②构造沉降作用对于湖泊沉积物的长期保存至关重要，水和沉积物可在无沉降区暂时保存，但这些沉积物难以保存在现今地层中。沉降型湖泊发育永久性可容纳空间，悬湖发育暂时性可容纳空间，虽然悬湖无法永久保存沉积物，但其临时储存的大量水体可以瞬时决口，淹没下游沉降型湖泊，这为富含有机物页岩的发育创造了有利条件。悬湖决口形成的洪水会导致下游沉降型湖泊发生大规模快速强制性湖侵（FT），从而形成了一种与正常水及沉积物供给无关的异整合面。

关键词: 湖相层序地层学, 欠填充湖泊, 平衡填充湖泊, 过填充湖泊, 强制性湖侵, 强制性湖退, 他旋回, 可容纳空间

Abstract:

Sequence stratigraphic concepts and methods provide novel tools for performing stratigraphic analysis, allowing us to improve our understanding of depositional models and basin evolution. Main controls and depositional elements (e.g. surfaces, systems tracts, parasequences, etc.) recognized in conventional sequence strati-graphy are designed for marine-related systems. In contrast, the sequence stratigraphy of lacustrine successions is much more complex, because it is not driven by sea-level changes, but by a complex interaction between tecto-nics and high-frequency climatic cycles. Through systematic analysis of lacustrine sedimentary systems, the re-levant concepts of lacustrine sequence stratigraphy were clarified. The controlling effects of allocyclic cycles on lacustrine sedimentation and sequence stratigraphy, accommodation space types of lacustrine basins and their significance for sequence stratigraphy and hydrocarbon genesis were explored.The results show that： （1） The lacustrine sedimentary conditions can be classified as three types: Underfilled, balanced-fill and overfilled lakes. There are significant differences in water salinity, sedimentary sequences, and system tracts under different lacustrine sedimentary conditions. Underfilled lakes are hydrologically closed lakes, and consequently, the lake-level can highly fluctuate, driven by high-frequency wet-dry climatic cycles. During wet periods, rivers supply water and sediments, resulting in fining-and thinning-upward elementary depositional sequences (EDS) accumulated during the transgressive systems tract (TST). In contrast, dry periods are characterized by a relative lake-level fall with the subaerial exposure of lake margin areas during the regressive systems tract (RST). Lake water salinity are brackish to hypersaline. Balanced-fill lakes are partially closed lakes, and consequently, they have characteristics of both underfilled and overfilled lakes. During the TST, the lake is in underfilled condition, and consequently, the introduction of water and sediment will accumulate a fining-upward interval until reaching the spill point during the maximum flooding. The RST is accumulated under an overfilled lake condition, with coarsening-upward progradational littoral deltas and related subaqueous delta deposits. Lake water salinity are brackish to freshwater. Overfilled lakes are hydrologically open lakes. Most deposits accumulate during the RST, forming coarsening-upward progradational littoral deposits, with associated subaqueous deltas. All overfilled lakes are freshwater lakes. （2） Subsidence is crucial for allowing the long-term preservation of lacustrine depo-sits. Lakes can temporarily store water and sediments in areas that lack subsidence, but these deposits will not be preserved in the stratigraphic record. Subsiding lakes develop permanent accommodation space and hanging lakes develop temporary accommodation space. Although hanging lakes cannot permanently store sediments,they can flood subsiding lakes with the near-instantaneous release of a substantial volume of water, creating favorable conditions for the accumulation of organic-rich shales. This rapid flooding from hanging lakes induced a forced transgression (FT), which is a large-scale rapid transgression (xenoconformity) not related to the normal sediment and water supply from local source areas.

Key words: lacustrine sequence stratigraphy, underfilled lakes, balanced-fill lakes, overfilled lakes, forced transgression, forced regression, allocyclic cycles, accommodation space

中图分类号: 

  • TE122.23

图1

湖相沉积层序发育的关键控制要素模式（据文献[38]修改）"

图2

基于可容纳空间与沉积物+水供给变化的湖盆类型划分（据文献[3-5,52]修改）"

图3

欠填充湖盆中相对湖平面变化与沉积层序特征（据文献[38]修改） (a) TST 期，河流流量增加，相对湖平面（RLL1→RLL3）上升，湖岸线（CL1→CL3）向陆地迁移；(b) TST 期，可容纳空间增大，发育向上变细变薄的沉积层序；(c) RST期，沉积物+水供给的减少导致强制性湖退，CL3→CL5，在广阔的湖缘区域形成暴露环境；(d) Wheeler图展示沉积作用随地质时间（t1—t5）的变化情况。"

图4

欠填充湖泊基本沉积序列（EDS）内部构成及形成机制（据文献[42]修改）"

图5

欠填充湖泊基本沉积序列（EDS）露头照片 （a） 渐进式湖侵过程中形成的向上变细EDS，底面为河流侵蚀面，中国滦平盆地白垩系西沟园组；（b） RST期间的恐龙足迹，表明湖泊几乎完全干涸，中国滦平盆地白垩系西沟园组；（c） 水体较浅的欠填充湖泊中发育多个呈叠加分布、向上变细变薄的EDS，阿根廷内乌肯盆地侏罗纪Tordillo组；（d） RST期间的泥裂现象，阿根廷内乌肯盆地的侏罗纪Tordillo组；（e） TST期发育的湖相页岩，顶部最大洪水面（mfs）之后进入RST，阿根廷内乌肯盆地的侏罗纪Tordillo组；（f） 小型EDS，显示为整体向上变细变薄的堆积模式，阿根廷Cuyo盆地三叠纪Potrerillos组。"

图6

平衡填充湖盆相对湖平面变化及沉积层序堆叠模式（据文献[38]修改） (a) TST 期，河流流量增加，相对湖平面上升，湖岸线（CL1→CL3）向陆地迁移；(b) TST 期，湖平面开始上升，形成由河道充填+朵叶体组成的退积序列；(c) RST期，湖平面到达溢出点，新输入沉积物形成了滨岸前积体，发生正常湖退，湖岸线CL3→CL5；(d) RST期，注入湖泊水量减少、蒸发作用增强和构造沉降作用导致相对湖平面（RLL）下降，在湖盆边缘区域形成强制性湖退；(d) Wheeler图，等时格架下不同沉积环境与沉积物分布特征，t1—t6为演化阶段，其中t1—t3对应TST期，t3—t6对应RST期。"

图7

平衡填充湖盆的基本沉积序列（EDS）内部构成及形成机制"

图8

鄂尔多斯盆地延长组平衡填充湖盆EDS露头照片 （a） EDS垂向特征，单个EDS表现为向上变细（TST）再变为三角洲前积体（RST）组成的沉积序列，最后以三角洲平原沉积结束，长4 + 5段；（b） RST和TST界线照片，层序边界处保存有原地生长的直立树木化石，长4 + 5段；（c） TST块状砂岩中直立树木化石照片，长4 + 5段；（d） 过填充期由异重流水下三角洲形成的厚层块状砂岩，长3段，TST期发育的厚层砂岩对底部前一期RST顶面细粒沉积有侵蚀冲刷；（e） 图d的局部放大图，厚层块状砂岩体底部存在冲刷侵蚀现象，发育叠瓦状斜列的泥砾，指示定向水流方向，长3段。"

图9

过填充盆地主要沉积特征和沉积模式（据文献[38]修改） (a) TST 期相对湖平面保持稳定；(b) RST 期，高沉积物供给导致正常湖退（湖岸线CL1→CL3），形成了由滨岸三角洲和相关水下三角洲沉积物组成的前积层序，相对湖平面降低；(c) TST期，沉积物供应减少，沉降作用促使湖盆可容纳空间增大，湖岸线CL3→CL4，相对湖平面升高，有利于湖盆深部富有机质页岩的发育；(d) RST期正常湖退，湖岸线CL4→CL6，沉积物供给再次增加，形成新的三角洲前积层；(e) 沉积作用随地质时间（t1—t6）变化的Wheeler图。"

图10

过填充淡水湖盆河流载荷类型与沉积特征"

图11

过填充湖盆基本沉积序列（EDS）内部构成及形成机制"

图12

陆相盆地沉积演化控制因素模式"

图13

气候对欠填充湖盆基本沉积序列的控制作用 注：RLL1→RLL3为相对湖平面由低至高。"

图14

他旋回对过填充湖盆基本沉积序列的控制作用"

图15

湖平面变化与强制性湖侵、湖退关系示意图"

图16

鄂尔多斯盆地三叠系延长组7段最大湖泛期湖盆溢出点及外流河谷形成示意图 （a） 长7最大湖泛期示意图，相对湖平面位置到达盆地溢出点附近；（b） 湖盆在溢出点附近发生决口、侵蚀下切形成外流河谷，导致湖平面迅速下降、形成强制性湖退；（c）和（d）均为长7段顶部的下切外流河谷沉积全景图，该外流河谷向下切割到长7段前三角洲泥岩上，推测湖平面下降了约15 m。"

图17

陆相盆地沉积体系中的暂时性可容纳空间和永久性可容纳空间示意图 注：EDS. 基本沉积序列；SB. 层序边界；FT. 强制性湖侵。 （a） 暂时性可容纳空间使得悬湖中蓄积一定量水体，欠填充湖盆发育向上变细变薄的EDS；（b） 悬湖决口形成大量洪水淹没下游沉降型湖盆，使其发生强制性湖侵，原源汇河流体系被淹没，形成欠补偿湖泊。"

图18

陆相湖盆中发育的典型强制性湖侵面露头照片 （a） 阿根廷库约盆地上三叠统Cacheuta组黑色富有机质页岩，下伏Potrerillos组为粗粒碎屑沉积物，上覆Rio Blanco组红色页岩，地层界线明显；（b） 阿根廷库约盆地Potrerillos组和Cacheuta组之间沉积相突变接触面，可被解释为由强制性湖侵或灾难性洪水事件引发形成的异整合面（Xenoconformity），Cacheuta组富有机质页岩中常夹凝灰岩层；（c） 阿根廷库约盆地Cacheuta 组黑色页岩和Rio Blanco组红色页岩沉积相突变接触面，该突变面也是异整合面，与强制性湖退及湖盆从欠填充到平衡填充的转化有关；（d） 鄂尔多斯盆地上三叠统延长组7段底部强制性湖侵界线处照片；（e） 鄂尔多斯盆地长7段紧邻强制性湖侵界线下方的植物根系层，表明暴露于空气中陆地环境突然被灾难性洪水所淹没；（f） 鄂尔多斯盆地长7段富有机质页岩与凝灰岩互层，表明沉积速率较低。"

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