A Lacustrine Basin Driven by Extreme Events of Alternate Dry-Wet Climatic Cycles: Evidence from Outcrops of Yanchang Formation in Upper Triassic, Ordos Basin
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摘要: 鄂尔多斯盆地是我国陆上最主要的油气盆地之一，三叠系延长组是该盆地的主要含油层位.通过对延长组典型露头的考察与研究，结合古生物及岩性岩相资料，取得了3点新认识：（1）恢复了延长组沉积时期的古气候环境，认为其具有三分性，其中早期拉丁期为干旱环境；中期受卡尼期梅雨事件（CPE）影响气候发生突变，转变为温暖潮湿气候环境；晚期诺利—瑞替期再次转变为半干旱—半湿润气候环境.（2）CPE事件改变了延长组沉积物搬运与沉积方式，其中CPE事件之前与事件之后的干旱环境时期，主要发育暴雨洪水引发的季节性河流、决口扇、决口河道沉积；CPE事件当中及卡尼中期，陆源碎屑物质主要通过异重流、浊流及砂质碎屑流等多种途径搬运至水下环境，形成富砂质重力流事件沉积，同时受CPE事件控制，在深水环境还发育了黑色富有机质页岩事件沉积.（3）建立了延长组干旱与潮湿两种环境沉积模式，干旱环境湖泊水域面积较小，主要沉积单元为洪泛平原、季节性河道及决口扇，主要沉积方式为填平补齐、加积式沉积，不发育前积沉积现象；潮湿环境湖泊水域面积较大，发育完整的陆相河流—三角洲—湖泊—重力流沉积体系，由于具有稳定的长流水，河道相对固定，加之受湖平面变化控制，其沉积方式以前积作用为主.该认识不仅对于深入探讨鄂尔多斯延长组大型坳陷湖盆形成演化机理、沉积层序充填演化及指导油气勘探实践有积极意义，而且对揭示晚三叠世全球极端气候事件在内陆湖盆的沉积学记录有积极意义，可以填补CPE事件在古特提斯东缘泛大陆内部沉积响应研究的空白.Abstract: The Ordos Basin is one of the main petroliferous basins in China. The Triassic Yanchang Formation is the main oil-bearing units in this basin. Based on the investigation and study of typical outcrops of Yanchang Formation and the data of paleontology, lithology and lithofacies, three new insights are obtained. (1) The paleoclimatic environment of Yanchang Formation during the sedimentary period has been recovered, which is considered to be tripartite, and the Ladinian Age was an arid environment. During the Carnian Age, the climate changed to a warm and humid environment because of the Carnian Pluvial Episode (CPE). In the Norian-Rhaetian ages, the climate environment changed to semi-arid and sub-humid again. (2) The CPE changed the way of sediment transport and deposition in the Yanchang Formation. In the dry environment period before and after the CPE, the seasonal river, crevasse splay and crevasse channels caused by rainstorm and flood were mainly developed. During the CPE and in the mid-Carnian period, terrigenous detrital materials were transported to the underwater environment mainly by various gravity flows such as turbidity flow, sandy debris flow and hyperpycnal flow, forming sandy event deposits. At the same time, controlled by the CPE, black organic-rich shale event deposits were also developed in the deep water environment. (3) Two sedimentary models of arid and humid environments were established in the Yanchang Formation. In the former, the catchment area in the arid environment was small, and the main sedimentary units were flood plain, seasonal channel, crevasse splay, crevasse channels and so on. In the latter, the catchment area of the humid environment is large, and the complete continental fluvial, delta-lacustrine and gravity flow sedimentary system is developed. Due to the stable long-flowing water, the channel is relatively fixed, the sedimentation mode is mainly progradation, supplemented by retrogradation, and not obvious aggradation. The study is of practical value to the discussion of how the large depressed lake basin formed and evolved in the Yanchang Formation, sedimentary sequence evolution, and petroleum exploration, and it is also significant to the study of the sedimentological records in inland lake basins generated by global extreme climate events in the Late Triassic Epoch to understand the sedimentary responses of the Carnian Pluvial Episode in the Pangea at the east margin of the Paleo-Tethys.
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图 1 鄂尔多斯盆地晚三叠世古地理位置、构造单元与延长组地层发育情况
a.盆地现今构造单元及黑色泥页岩残留分布；露头：1.延河，2.仕望河，3.铜川衣食村，4.窟野河；①为阿尼玛卿‒商丹断裂带，②为西六盘山断层，③为东贺兰山断层. b.晚三叠世盆地位置（据Bai and Ma, 2020修改）. c.延长组岩性岩相综合柱状图
Fig. 1. Late Triassic paleogeographic location, tectonic units and stratigraphic development of Yanchang Formation in Ordos Basin
图 3 延长组沉积时期孢粉植物群主要类型分布与古气候演化
长10油层组及纸坊组中未发现孢粉化石
Fig. 3. Distribution of the main types of palynological flora and paleoclimate evolution during the deposition of Yanchang F ormation
图 4 陕北地区延长组露头剖面典型古土壤层照片
a. 干旱环境古土壤，延河剖面长9内部；b. 照片a的局部放大，土黄色粉砂质泥岩，层理杂乱，见稀疏植物根系，上覆炭质泥岩；c. 潮湿环境古土壤层，延河剖面长7顶部；d. 照片c的局部放大，黑色泥质粉砂岩，层理杂乱或不显层理构造，见大量垂直生长植物根系、虫孔等；e. 干旱环境古土壤，深褐色、杂色含钙质结核粉砂质泥岩，仕望河剖面长10中部；f. 照片e的局部解释；g. 干旱环境古土壤，延河剖面长61底部；h. 干旱环境古土壤，延河剖面长4+5中部.照片的位置见图 2
Fig. 4. Photos of typical paleosol layers in the outcrop profile of Yanchang Formation in northern Shaanxi
图 5 白家河地区延长组长9油层组岩性岩相特征
a.实测柱状图(厚度49.2 m): b.露头宏观照片: c.落石, 浅灰绿色砂岩, 其下部为块状, 向上略显交错层理, 位置见照片b; d.照片c的底面, 见大量炭化植物茎秆与叶片指示洪水事件; e照片e的顶面，见大量类似*龟甲纹状”多边形裂缝, 疑似干裂现象.CVS.决口扇; FP.洪泛平原; CCH.决口河道
Fig. 5. Lithologic and lithofacies characteristics of Chang 9 oil formation in Baijiahe area
图 6 冯家村-胡家村长4+5油层组岩性岩相特征
a.实测柱状图(厚度26 m); b.露头宏观照片; c、d.照片b的局部放大, 显示了两颗原地生长的直立树木化石, 其宿主岩石为含泥质粉细砂岩(局部见油苗), 块状层理, 底面平直, 显示为沉积速率很高的决口扇沉积.CVS.决口扇砂体
Fig. 6. Lithology and lithofacies characteristics of Fengjiacun- Hujiacun Chang 4+5 reservoir
图 7 黑家堡村长3油层组岩性岩相特征
a.实测柱状图(厚度46 m); b.露头宏观照片; c、d、e、g、h.地层中直立分布的树木化石，树木根系部分埋藏在暗红色粉砂质泥岩中，泥岩中发育垂直虫孔等大量生物遗迹化石，显示为洪泛平原微相，茎干部分宿主岩石为含泥质粉细砂岩, 块状、无层理，底面平直, 显示为沉积速率很高的决口扇沉积, 由此推测这些树木当时位于河流末端低洼处，因洪水决口掩埋而成化石，其中照片c中的树木经过了两次掩埋，其余均为一次性掩埋; f.照片e的解释.图中红色五角星指示树木化石分布地点.CVS.决口扇; FP.洪泛平原: CCH.决口河道
Fig. 7. Lithology and lithofacies characteristics of Chang 3 reservoir in Heijiapu Village
图 8 延河剖面二里畔村长7/长8地层界线附近的沉积相突变现象
a. 露头宏观照片；b、c. 照片a的局部放大，浅灰绿色泥质粉砂岩中见炭化植物茎秆及大量垂直植物根迹等生物扰动构造，顶部发育薄层劣质煤线或炭质泥岩，指示为浅覆水沼泽或三角洲平原环境；d. 长7/长8之间的沉积相突变界线，其中界线之下长8为暴露古土壤层，界线之上长7为深湖‒半深湖相油页岩沉积，位置见照片a；e~g. 照片d的局部放大，古土壤层，厚度10~15 cm，浅灰绿色泥质粉砂岩中见原地生长的树干化石及大量垂直生长的植物根系，由于遭受生物高度扰动，岩石呈松散状，无常规层理构造；h. 照片d的局部放大
Fig. 8. Abrupt change of sedimentary facies near the stratigraphic boundary of Erlipan Village Chang 7/Chang 8 in Yanhe Section
图 9 铜川剖面长8-长7段岩性剖面（实测）及典型现象露头照片
a. 铜川地区实测岩性剖面；b. 油页岩夹薄层凝灰岩，长7中部；c. 重力流砂体夹薄层油页岩与黑色泥岩，长7上部；d. 长7/长8之间的沉积相突变界线，其中界线之下长8为三角洲洪泛平原沉积，界线之上长73底部为深湖‒半深湖相油页岩，局部夹几厘米到十几厘米厚度不等薄层凝灰岩，向上部变为重力流砂体与油页岩互层；e、f. 照片d的局部放大，浅灰绿色泥质粉砂岩中见垂直生长的植物根系及垂直生物钻孔等，由于遭受生物高度扰动，岩石呈松散状，无常规层理构造.照片的位置见图 9a
Fig. 9. Lithologic profile and outcrop photos of typical phenomena of Chang 8-Chang 7 members in Tongchuan Section
图 10 鄂尔多斯盆地延长组沉积模式
据李相博等(2021a, 2021b)修改. a. 干旱时期的河流扇沉积模式：在干旱环境下，陆相盆地湖泊水域面积较小，主要沉积单元为洪泛平原、河道与决口扇（决口河道），河流扇中的“扇状沉积体系”主要由洪水期曲流河决口、改道迁移而形成，一般缺少明显前积现象；b. 潮湿时期的湖泊‒三角洲‒重力流模式：在潮湿环境下，陆相盆地湖泊水域面积大，主要沉积单元有河流、三角洲、深湖‒半深湖及重力流沉积，在三角洲前缘发育明显前积体.1.河道砂体；2.沿岸沙坝；3.近岸沙坝；4. 河口坝；5.远沙坝；6.席状砂；7.风暴岩；8.砂质碎屑流；9.浊流；10.异重流；11.底流
Fig. 10. Depositional model of Yanchang Formation in Ordos Basin
表 1 延长组卡尼期岩性岩相类型、成因解释及其鉴别标志
Table 1. Lithologic lithofacies types, genetic interpretation and identification marks of Carnian period in Yanchang Formation
类型划分 沉积特征 搬运与沉积过程 岩性岩相 代码 岩石结构 沉积构造 单岩层厚度 顶底接触关系 沉积相序 典型照片 流体类型 搬运过程 沉积机制 交错-平行层理砂岩相 L1 砂级-粉砂级-泥级，概率曲线由滚动、跳跃及悬浮三段式构成 砂岩内部发育交错层理、平行层理、沙纹层理等牵引流沉积构造，砂岩底部可见泥砾等冲刷现象 变化较大，最大可达几十米 底面为冲刷面，顶面有时为泥岩，但常为冲刷面 
B209井, 2 060.0~2 080.3 m
B210井, 1 894.5 m牵引流、流体重力流(Shanmugam, 2013) 底床搬运为主(Shanmugam, 2013) 机械分异、重力沉积(Shanmugam, 2000) 块状层理砂岩相 L2 砂级-粉砂级，概率曲线为两段式，以跳跃为主，C-M图平行于C=M基线 块状层理，砂岩内部偶见呈悬浮状零散分布泥砾, 且有拖长变形现象 一般大于0.5 m，最大可达几十米 顶底面均突变接触，其中底面平坦，顶面为不规则状 
N36井, 1 571.6~1 574.3 m
N36井, 1 572.4 m宾汉塑性体，层流
(Shanmugam, 2013)块体搬运(Shanmugam, 2013; Stow and Johansson, 2000) 整体冻结(Talling et al., 2012; Shanmugam, 2013) 薄层正粒序砂岩相 L3 砂级-粉砂级-泥级，概率曲线为单段式，斜率小，C-M图平行于
C=M基线粒序递变层理或含有粒序层理的鲍玛序列. 通常小于0.5 m 底面常见槽模等侵蚀冲刷现象，顶面为渐变界面 
N36井, 1 514.6~1 514.8 m
N36井, 1 514.8 m牛顿流体，紊流(Bouma, 1962; Shanmugam, 2013) 流体搬运
(Bouma, 1962; Shanmugam, 2013)悬浮析出(Shanmugam, 2013) 正反粒序成对产出砂岩相 L4 砂级-粉砂级-泥级，概率曲线为单段式，斜率小，C-M图平行于
C=M基线正粒序递变层理与反粒序递变层理成对出现，单砂层内有微冲刷现象. 单层小于20 cm 顶底面均突变接触 
JH4井, 1 446.97~1 447.36 m
JH4井, 1 446.97~1 447.36 m异重流（Mulder and Alexander, 2001; Zavala and Arcuri, 2016; Yang, 2017) 悬浮搬运、底床搬运(Zavala and Arcuri, 2016; Yang, 2017) 悬浮析出与机械分异(Zavala and Arcuri, 2016; Yang, 2017) 砂泥混搅相 L5 砂到泥级 强烈揉皱变形层理, 发育压力脊，滑坡壁，压力缝等 变化较大 顶底面均突变接触 
B414井, 1 985.0~1 988.0 m
B280井, 1 906.6 m砂质滑塌、滑动(王德坪, 1991; Talling et al., 2012) 块体搬运(王德坪, 1991; Talling et al., 2012) 整体冻结(Shanmugam, 2013) 无层理构造泥岩相 L6 泥级为主 块状，通常见疙瘩状或透镜状团块，有时见粉砂质或泥质撕裂屑 单层常小于
30 cm顶底面均突变接触 
长63, 铜川剖面
长63, 铜川剖面泥质碎屑流(王德坪, 1991; Talling et al., 2012) 块体搬运(王德坪, 1991; Talling et al., 2012) 絮凝或整冻结体(王德坪, 1991; Talling et al., 2012) 水平层理泥岩相 L7 泥级为主 浅灰、灰黑或深黑色，发育水平层理，常与L1-L4相伴生，形成韵律层理 变化较大 与上、下两层呈渐变或突然接触 
长7, 铜川剖面
长7, 铜川剖面静水环境(Talling et al., 2012) 流体浮力(Talling et al., 2012) 悬浮析出(Talling et al., 2012) 
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