Constraints of hydrodynamic conditions on gas reservoirs in Dongying depression and its enlightenment to CO2 storage target area
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摘要:
东营凹陷及周边大量的天然气藏预示着这些区域具有良好的CO2地质封存条件。为了优选出东营凹陷及周边适宜CO2封存的靶区，通过收集资料与盆地流场综合分析，总结归纳了东营凹陷及周边埋深为500～1500 m的天然气成藏的主控因素、赋存模式，以及东营凹陷地下流体动力场对天然气藏形成的制约作用。研究结果显示：（1）按照地下流体运动特征与方式，天然气藏形成的输导方式可划分为侧向型输导体系与垂向型输导体系，侧向型主要分布在凹陷边缘高凸起带，垂向型主要分布在盆内凹陷区。（2）压实流是凹陷中心的深部气源向上运移的主要驱动力，一部分深源气体自凹陷中心向凹陷边缘产生较长距离的运动，在凹陷边缘的高凸起部位压实流与重力流的接合区形成封闭的水动力圈闭，形成侧向型天然气藏；另一部分深源气体在压实流驱动下，沿高孔渗断裂带垂向运移进入顶部的圈闭中聚集成藏。由于断层错断导致的岩性圈闭比较发育，与水动力圈闭一起构成气体的有效圈闭，形成垂向型天然气藏。（3）东营凹陷CO2封存最有利靶区主要位于凹陷西、北方向的青城凸起、林樊家凸起、滨县凸起、陈家庄凸起、广饶凸起等高凸起及其周边；东部的广饶凸起、青坨子凸起等凸起及凹陷区的垂向断裂发育区为CO2封存较有利靶区。研究认识对我国东部沉积盆地高碳排放区CO2地质封存场地优选具有参考意义。
Abstract:A large number of natural gas reservoirs in Dongying depression and its surrounding areas indicate that there are good conditions for CO2 geological storage in these areas. To optimize the target area suitable for CO2 storage, through data collection and comprehensive analysis of Dongying basin flow field, this study summarized the main controlling factors and occurrence modes of natural gas accumulation in Dongying depression and its surrounding areas with a buried depth of 500-1500 m, and analyzed the restrictive effect of underground hydrodynamic field on the formation of natural gas reservoirs. The results show the migration pathways of shallow gas reservoirs can be divided into lateral migration pathways and vertical migration pathways based on the characteristics and modes of underground fluid movement. The lateral type is mainly distributed in the high uplift belt at the edge of the depression, and the vertical type is mainly distributed in the depression area in the basin. Compaction flow is the main driving force for the upward migration of the deep gas source in the center of the depression. A part of the deep gas moves for a long distance from the center of the depression to the edge of the depression, forming a closed hydrodynamic trap and a lateral shallow gas reservoir at the junction of compaction flow and gravity flow in the high convex part of the edge of the depression. The other part of deep gas, driven by compaction flow, migrates vertically along the high porosity and permeability fault zone and accumulates in the trap at the top. Lithologic traps caused by fault dislocation are relatively developed, which together with hydrodynamic traps form an effective trap of gas and form a vertical shallow gas reservoir. The most favorable target area for CO2 storage in the shallow part (500-1500 m) of Dongying depression is mainly located in the west and north direction of the depression, such as Gaoqing Uplift, Linfanjia Uplift, Binxian Uplift, Chenjiazhuang Uplift, Guangrao Uplift, and their surrounding areas. The vertical fault development areas of Guangrao uplift, Qingtuozi uplift, and other depressions in the east are favorable targets for CO2 storage in the shallows.
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CO2地质封存（geological CO2 sequestration， GCS）是指模仿化石能源的埋存，在类似的地质结构中把从地下开采出来的碳再放回到地下[1]。GCS的主要场所包括枯竭油气藏、不可开采煤层和深部咸水含水层。其中深部咸水含水层是封存场地广泛和封存效果最好的场所，根据张洪涛等[2]、李小春等[3]的估算，中国CO2地质潜力封存量巨大，其中以深部咸水层封存量为主，完全可满足我国CO2地质封存使用。GCS是实现碳达峰、碳中和的主要地质路径[4]，也是能够有效减少大型工业碳排放的手段，它将分担未来大约14%的全球碳排放量来满足巴黎协定“2 °C目标”[5]。
封存效果是GCS最受关注的问题[6]。因此，我国研究者在优选CO2地质储存场所时，均将盖层封闭性、封存体稳定性、水动力封闭（封堵）作用等作为靶区筛选的主要指标[7 − 10]。CO2在深部咸水含水层中的封存机理包括构造与地层封存/水动力封存、毛细封存、溶解封存和矿化封存等[11 − 12]；涉及多个复杂的地质过程，包括多相多组分的运移过程、储层热响应、地下流体动力场、水岩相互作用和地质力学变化等。咸水层CO2地质封存本质上相当于寻找或营造一个地下“人工气藏”[13]，这就为我们提供了一个思路：可以根据天然气藏的有利构造部位与赋存地质条件，寻找类似地质条件的地质构造部位，作为GCS的有利场所。
东营凹陷是我国重要的油区，不但发现了大量油田，也发现了大量伴生气藏[14 − 15]，气藏以高含CH4为主，少量为高含CO2气藏。尤其是埋深为500～1 500 m的天然气藏[16 − 17]的赋存规律，对咸水层CO2浅部地质封存具有重要的启示意义，可以选取与天然气藏所处类似地质条件的构造部位，作为咸水层CO2地质封存的靶区，以实现较好的CO2封存效果。本文全面分析研究了前人关于东营凹陷及周边天然气藏的研究成果和天然气成藏的主控因素及模式，特别是重点分析地下流体的运移规律、水动力条件与圈闭作用对CO2地质封存的控制作用，在此基础上，优选出东营凹陷及周边适宜CO2地质封存的靶区，为东部高碳排放区CO2封存场地选择提供参考。
1. 地下流体动力场对天然气藏赋存的控制作用
东营凹陷位于渤海湾盆地济阳坳陷的东南部，东西长约100 km，南北宽约64 km，面积5700 km2。东营凹陷是一个含天然气丰富的负向构造单元，四周以隆起或凸起为界：东为垦东凸起、青坨子凸起，北为陈家庄凸起，西为滨县凸起和青城凸起，南面的鲁西南隆起既是东营凹陷的南界，也是济阳坳陷的南界（图1）。
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1.1 天然气藏分布特征
天然气田主要分布于东营凹陷的边缘、凹陷与周边凸起的接合部位，埋深为500～1 500 m。如青城凸起的花沟气田，滨县凸起、林樊家凸起顶部的气藏，陈家庄凸起南北两侧的盐家气田与三合村气田等（图1），沿东营凹陷的边缘基本呈环状分布[14]。
（1）垂向分布
东营凹陷已发现的探明的含气层位自下而上为前震旦系、中生界、新生界的孔店组、沙（河街组）四段、沙三段、沙二段、沙一段、东营组、馆陶组和明化镇组共10套含气层系。埋藏深度628.6～1 848.0 m，主要气藏的埋藏深度为800～1 500 m。含气层系多、埋藏浅是东营凹陷气藏分布的显著特点。
（2）横向分布
东营凹陷天然气的储集分为溶解气、气顶气、纯气藏三种状态[14]。这三种状态的天然气在凹陷中的分布具有明显的规律性，自凹陷内部到凹陷边缘天然气可分为三个环形分布区。一为油藏中的溶解气，分布于东营凹陷的中心区；二为油藏顶部的气顶气，分布于中心区的外围；三为纯气藏，主要分布于东营凹陷边缘的凸起部位（图1）。
1.2 沉积盆地地下流体动力场对气藏形成的控制
东营凹陷及周边气藏既有无机成因又有有机成因，其中高含CO2气藏以无机成因为主[16 − 17]。油气的运移、聚集与地下流体动力场的分布规律紧密相关，从流体动力学的角度分析，油气可以在不同的局部水动力环境中聚集[18]。
在厚度巨大的松散碎屑岩类沉积盆地中，一般均存在着两种不同成因的地下水动力系统，一种是渗入成因，另一种是沉积成因水[19]。含油气盆地水文地质的相关研究认为[20−21]，大型沉积盆地地下水动力系统由大气降水渗入成因水和沉积成因水共同组成，具有区域性的水力连续性或统一的水力联系。渗入成因水在重力作用下，沿盆地边缘流向盆地中心或地势较低的盆地另一侧边缘，因此表现为“向心流”；沉积成因水主要来自于盆地内沉积物经压实而被排挤出来的水（即压实流），其流向从盆地沉积中心向周边呈放射状流动，表现为“离心流”。两种不同成因、不同流向的地下流体，在盆地一定部位形成动力平衡[19]。
含油气流体自凹陷中心的地层高压区（压力系数>1.2）[22]沿孔隙度较高的含水层与导水性能较好的断层，向凹陷边缘的常压区（压力系数<1.0）流动，携带着油气的压实流与来自补给区的循环深度较浅（一般在3 000 m以浅）的渗入水相遇，形成封闭的地下流体动力平衡环境，在浮力或压差作用下向顶部运移，并发生重力分异[23 − 24]，在有利的构造圈闭部位形成气藏（图2），动力平衡区流体一般表现为高矿化咸水特征[19]。
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图 2 东营凹陷油气藏差异富集及水动力特征（剖面位置见图1）（据文献[22]修改）注：Nm—新近系明化镇组；Ng—新近系馆陶组；Ed—古近系东营组；Es1—古近系沙河街组一段；Es2—古近系沙河街组二段；Es3—古近系沙河街组三段；Es4—古近系沙河街组四段；Ek——古近系孔店组。下图同。Figure 2. Differential enrichment and hydrodynamic characteristics of oil and gas reservoirs in Dongying depression (see fig. 1 for profile position) (modified after Ref. [22])2. 气藏的形成赋存方式
天然气藏的形成研究成果比较丰富，按促使其形成的地下流体运动的主要方向，可划分为侧向型输导体系与垂向型输导体系[25 − 27]。侧向型输导体系重点在于量化表征骨架砂体对于天然气的输导能力，而垂向型输导体系则表现为断裂的垂向活动特征对于天然气运移的影响。
2.1 侧向型输导体系
浅层气藏多分布于东营凹陷的边缘高凸起部位，含气流体主要是在压实流的控制下，从凹陷中心沿孔隙度较高的含水层向侧上方盆地边缘的凸起运移，压实流流体势逐渐变弱，遇到循环深度较浅的重力流则形成封闭的地下流体动力平衡区，在合适的构造圈闭部位形成浅部气藏，其圈闭类型主要为水动力圈闭（图3）。输导砂体与古地貌的叠合，明确了侧向型浅层气输导体系骨架砂体的分布特征，为侧向型输导模式的建立奠定了基础[28]，如青城凸起的花沟气田、林樊家凸起的林樊家气田、滨县凸起的单家寺气田等（图1）。
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2.2 垂向型输导体系
深部沉积成因水不仅沿储层进行侧向运移，在导水断裂构造发育的情况下，深部的沉积成因水还会沿断层向浅部作垂向运移，渗透到较浅部的渗入成因水中，在盖层和重力流配合下，CO2向上扩散时将被地下水封堵，在合适的构造部位形成浅部气藏（图4）。其圈闭类型主要为水动力圈闭和岩性圈闭，其中岩性圈闭是因为断层错断导致储层与隔水层对接而形成的圈闭[29]，主要分布于凹陷区内垂向断裂比较发育的构造部位，如三合村气田、盐家气田等（图1）。
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3. CO2气藏形成赋存模式与封存有利靶区
3.1 CO2气藏形成赋存模式
综上所述，东营凹陷的CO2气藏的形成赋存模式主要分为侧向型和垂向型2种。
侧向型输导模式可归纳为：凹陷中心的深部气源在压实流驱动下，通过储层的骨架砂体向盆地边缘侧向上运移，通过断层的垂向沟通进入凸起带，使得天然气进一步向高部位运移。同时天然气还可穿越泥岩盖层垂向运移之后进入上部层组砂体中，进入有效圈闭聚集成藏。在压实流与重力流的接合区形成封闭的地下流体动力平衡区（即水动力圈闭），为主要的圈闭方式（图5）。气藏赋存层位主要为埋藏较浅的新生界明化镇组、馆陶组、东营组砂体。
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垂向型输导模式可归纳为：凹陷中心的深部气源在压实流驱动下，进入相对较高渗透性的断裂带内，天然气沿断裂带垂向运移进入顶部的圈闭中聚集成藏。由于高孔渗断裂带的存在，使得在垂向型输导模式中天然气穿越盖层垂向运移的概率较低，主要沿断裂带垂向运移。由于断层错断导致的岩性圈闭比较发育，与水动力圈闭一起构成气体的有效圈闭（图5）。气藏赋存层位为气源层之上的砂体。
馆陶组顶部—明化镇组底部泥岩组成区域性盖层，累积厚度350～500 m，尤其明化镇组泥岩是阻止油气散失的最后一道屏障，构成东营凹陷天然气藏成藏的良好盖层[31 − 32]。
3.2 东营凹陷CO2封存靶区
根据以上CO2气藏形成赋存模式，可大致判断出东营凹陷CO2封存的靶区。东营凹陷周边的高凸起部位，为压实流与重力流的水动力平衡区，流体运动滞缓，是气体长期贮存的有效圈闭区，也是CO2封存的有利靶区。由于重力流的流动方向主要是自南、西、北3个方向向东流动，所以CO2封存靶区主要位于东营凹陷的南、西、北3个方向的青城凸起、林樊家凸起、滨县凸起、陈家庄凸起、广饶凸起等高凸起靠近凹陷的部位（图6）。同时，在凹陷区的垂向断裂发育区，由于断裂错断形成的岩性圈闭比较发育，CO2封存靶区需要根据具体地质构造发育情况确定。
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因此，判断位于重力流主要来水方向的西部、北部的青城凸起、林樊家凸起、滨县凸起、陈家庄凸起及周边为CO2封存的最有利靶区，东部的广饶凸起、青坨子凸起等凸起及凹陷区垂向断裂发育区为CO2封存的较有利靶区。
当然，对于具有开发意义但尚未开发的天然气藏，不宜直接用来进行CO2地质封存。对于那些具备了CO2气藏形成赋存地质条件的构造部位，但缺乏气源而没有形成气藏的区域，或者已经开发完成的枯竭气田[35]，是当前可用于CO2地质封存的有利靶区。
4. 结论
（1）根据东营凹陷地下流体动力场特征及其运动的主要方向，将气藏形成的输导方式划分为侧向型输导体系与垂向型输导体系。侧向型主要分布在凹陷边缘高凸起带，垂向型主要分布在盆内凹陷区。
（2）压实流是凹陷中心深部气源向上运移的主要驱动力。一部分深源气体自凹陷中心向边缘产生较长距离的运动，在凹陷边缘高凸起部位压实流与重力流的接合区形成封闭的水动力圈闭，形成侧向型天然气藏。另一部分深源气体在压实流驱动下，沿高孔渗断裂带垂向运移进入顶部的圈闭中聚集成藏，由于断层错断导致岩性圈闭比较发育，与水动力圈闭一起构成气体的有效圈闭，形成垂向型天然气藏。
（3）东营凹陷CO2地质封存最有利靶区主要位于凹陷西、北方向的青城凸起、林樊家凸起、滨县凸起、陈家庄凸起、广饶凸起等高凸起及其周边。东部的广饶凸起、青坨子凸起等凸起及凹陷区的垂向断裂发育区为CO2地质封存较有利靶区。
需要提出的是，本文主要是从地下流体的水动力条件及地质圈闭作用这一角度来确定CO2地质封存的有利靶区，而CO2地质封存有利靶区的综合确定，还要全面分析CO2储存容量、技术成熟度、经济适宜性、地质安全、生态环境和社会意识等。
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图 2 东营凹陷油气藏差异富集及水动力特征（剖面位置见图1）（据文献[22]修改）
注：Nm—新近系明化镇组；Ng—新近系馆陶组；Ed—古近系东营组；Es1—古近系沙河街组一段；Es2—古近系沙河街组二段；Es3—古近系沙河街组三段；Es4—古近系沙河街组四段；Ek——古近系孔店组。下图同。
Figure 2. Differential enrichment and hydrodynamic characteristics of oil and gas reservoirs in Dongying depression (see fig. 1 for profile position) (modified after Ref. [22])
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图 6 东营凹陷CO2咸水层地质封存靶区分布（图中沙四段上压力系数等值线据文献[33]，重力流、压实流据文献[34]。）
Figure 6. Distribution of geological storage targets in shallow saline water layer of CO2 in Dongying depression (The isoline of pressure coefficient on the fourth member of Shahejie Formation is adapted by Ref. [33] ,and the gravity flow and compaction flow are adaptet by Ref. [34].)
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