Geological significance, prediction, and application of structural fractures in tight limestone reservoirs of the Taiyuan Formation in Ordos Basin
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摘要: 鄂尔多斯盆地太原组灰岩分布范围广泛，厚度大，但因岩性致密，单井产量低，长期以来天然气勘探未获得重大突破。随着研究的深入，发现高产气流井储层段往往受构造裂缝发育程度的控制。对于构造缝是否与储集层的优劣、天然气的成藏富集有关，以往缺少系统分析。本次研究首次系统总结了太原组灰岩构造缝特征，通过单轴载荷下岩石核磁共振（NMR）、CT扫描等技术分析了构造裂缝对储层的影响，剖析了缝网系统在成藏过程中的输导作用，根据研究区地质背景构建了改进的高斯曲率法（IGC）预测有利构造缝的发育区，并在横山地区井位部署中应用。结果表明：1）相对低角度缝、斜交缝，高角度张裂缝充填程度低，有效性好，常贯穿、切割、错动其它类型的裂缝使灰岩储集性能变好，同时形成的缝网系统利于烃类的高效运移；2）构造缝对致密灰岩储层物性有极大贡献作用，岩石物理实验表明，在裂缝发育的情况下，平均孔隙度由2.1%增加到4.2%，增加1倍。裂缝对总孔隙度的贡献率在14.3%~72.7%，平均值43.4%，三种储集岩性中，粉晶灰岩孔隙度增加最大、藻粘结灰岩次之，泥晶灰岩最小；3）改进的高斯曲率法（IGC）可预测有利构造缝的发育区，IGC值越大，高角度张性裂缝越发育，天然气富集条件越有利，该方法在横山地区取得了成功应用。上述认识将进一步指导盆地范围内太原组灰岩下一步的大面积勘探开发。Abstract:
In Ordos Basin,the Taiyuan Formation mainly consists of a marine-terrestrial transitional sedimentary system.The northern part featured shallow water delta deposits dominated by terrigenous clastic rocks, while the southern part consists of coastal marine limestone deposits. The Shenmu Gas Field has been discovered in the northern terrigenous clastic rock strata. The southern limestone strata has a wide distribution, covering approximately 14 square kilometers, and exhibits considerable thickness, ranging from 5 to 30 meters.However, the limestone reservoir is dense with an average porosity of 2.1%, an average permeability of 0.21mD, and an average throat radius of 0.12μm. For a long time, exploration had not focused on it due to its dense reservoir lithology.Recent years, further research has indicated that the high-yield gas wells are often related to the development degree of structural fractures.However, there is a lack of systematic analysis of whether the quality of the limestone reservoir and the natural gas enrichment relate to these structural development. To solve the above difficulties, the following steps have been studied and adopted in this study.Considering the tectonic setting,the structural fracture characteristics the of the Taiyuan limestone were firstly analyzed by field profiles, core observations, and well log data.Secondly the impact of structural fractures on the porosity of dense limestone reservoirs was observed by uniaxial loading rock core nuclear magnetic resonance (NMR) technology and CT scanning for the first time. Furthermore, the fluid inclusion was investigated to analyze the conducing role of the fracture networks during gas accumulation process.Lastly, based on the work mentioned above,to predict the development of structural fractures and favorable blocks exploration, an improved Gaussian curvature method (IGC) was proposed,according to the specific geological conditions, and it was applied in well deployment in the Hengshan area. The results show that: 1) In the study area, regional tectonic stress field is mainly influenced by the Yanshanian Movement,and the main tectonic framework was mainly established by it with NW-SE compressive stress.Compared with low-angle fractures and oblique fractures, high-angle tension fractures have low filling levels and good effectiveness.it often penetrates, cuts, and dislocates other types of fracture improving the limestone reservoir properties. In addition, the formed fracture network system may facilitate the efficient migration of hydrocarbons; 2) Rock physics experiments had manifested that structural fractures greatly contribute to the physical properties of the tight limestone reservoirs.With the development of fractures, the average porosity doubled from 2.1% to 4.2%. The contribution rate of fractures to total porosity ranged from 14.3%~72.7%, with an average of 43.4%. Among the three reservoir rock types, the porosity of powder crystal limestone increased the most, followed by algae bound limestone, and mud crystal limestone had the smallest increase; Combined with typical well reservoir-forming temperature, burial history, and thermal evolution history in the study area,inclusion analysis made clear that the widely developed fracture networks formed an effective transport system, and hydrocarbons effectively migrated by it during the main reservoir-forming period from the Late Jurassic to the Early Cretaceous.That is to say, generated from the main coal-bearing source rocks 8# coal and 5# coal located at the top and bottom of the limestone reservoir,the natural gas entered the limestone reservoir by the effective transport system.And supplemented by a cap rock of the marine mudstone on the top of the Taiyuan Formation, a superior "sandwich" type reservoir formed;4) The improved Gaussian curvature method (IGC) can predict the development degree of favorable structural fractures. The higher the IGC value, the more developed the high-angle tension fractures, and the more favorable the conditions for natural gas enrichment. This method was a debut in the Hongshan area to support well deployment. YT1H*,the first risk exploration well, achieved a gas production of 540,000 cubic meters per day, and marked a breakthrough in the exploration of the Taiyuan limestone in the Ordos Basin. In the past 2 years, 9 industrial gas wells have been discovered in this area, 5 of which have output above 100,000 cubic meters per day. Among them, YT4H* achieved an output of 1,088,000 cubic meters per day.The above exploration achievement demonstrated the effectiveness of the research and provided a reference for re reacquainting tight carbonate reservoirs. It is expected that this study can further guide the large-scale exploration and development of the Taiyuan Formation limestone in the Ordos Basin. -
Key words:
- Ordos Basin /
- Taiyuan Formation /
- Dense limestone /
- fractures prediction /
- Exploration Target Selection
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0. 引 言
鄂尔多斯盆地太原组主要为一套海陆交互相沉积体系，北部发育浅水三角洲沉积，以陆源碎屑岩为主，南部为陆表海碳酸盐岩沉积，具有“北砂南灰”的格局特点。太原组地层夹于主力烃源岩5#、8#煤层之间，具有良好的成藏组合条件（图1a）。长期以来对太原组的勘探及研究主要集中于北部的陆源碎屑岩地层[1−3]，并发现了神木大气田[4−6]。南部灰岩地层虽然分布范围广（图1b），约14 km2，而且有一定厚度5~30 m，但因其储层致密而未引起足够重视。在靖边奥陶系风化壳气藏勘探过程中，针对太原组气测显示较好的灰岩段进行了单层测试，仅有ZH2井、ZH3井等获工业气流，大部分单井产量低，所以针对太原组灰岩的勘探并未持续进行，未获得重大勘探突破。当时部分学者对太原组灰岩开展了研究，认为灰岩储层物性以特低孔、特低渗为特征[7−8]。近年来，中国石油长庆油田公司对太原组石灰岩这一潜在的天然气勘探新领域进行了重新探索[9]。随着研究的深入，发现高产气流井储层段往往受构造裂缝发育程度的控制。对于构造缝是否与储集层的优劣、天然气的成藏富集有关，缺少系统分析。本次研究首次系统总结了太原组灰岩构造缝特征，通过单轴载荷下岩石核磁共振技术（NMR）、CT扫描分析了构造裂缝对储层的影响，剖析了缝网系统在成藏过程中的输导作用，构建改进的高斯曲率法（IGC）预测有利构造缝的发育区，并在横山地区井位部署中应用。部署的YTH*测试达到108.8×104 m3/d的高产天然气无阻流量，展示了研究的有效性。期望该项研究能进一步指导盆地范围内太原组灰岩下一步的大面积勘探开发。
图 1 鄂尔多斯盆地太原组灰岩分布与地层特征（a）地层特征 （b）灰岩平面分布Figure 1. Distribution and stratigraphy characteristics of the Taiyuan Formation limestone in Ordos Basin(a)Stratigraphy characteristics;(b)Thicknes distribution of Taiyuan limestone1. 区域地质概况
晚奥陶世末，受加里东运动影响，鄂尔多斯盆地主体抬升为陆，结束了盆地海相碳酸盐岩沉积，并遭受了约1.4亿年风化剥蚀[10]；晚石炭本溪期，海水从东西两侧进入盆地，发育海相泻湖—潮坪沉积体系。后期，海水从东南方向缓慢退出，形成了广覆分布的8、9号煤层，厚5~20 m[11−12]；太原期，沉积环境表现为持续海侵与短暂海退，南北沉积差异明显，沉积古地形整体为北高南低，发育一套海相泻湖－潮坪—三角洲的海陆交互相沉积体系，形成了碳酸盐岩、煤层、陆源碎屑岩的混合建造。研究区处于陆表海潮坪环境，发育泥坪、混合坪、生屑滩、生物丘和灰坪5种微相类型，其中生屑滩、生物丘物性相对较好，是有利的沉积微相。生屑滩岩性以生屑粉晶灰岩（图2.a）为主，生物丘岩性以藻黏结灰岩（图2.b）为主，灰坪岩性以泥晶灰岩（图2.c）或泥质灰岩为主。灰岩矿物组成整体上以方解石主，脆性矿物达到91.3%，具有高脆性的特征。
图 2 鄂尔多斯盆地太原组灰岩储层特征（a）生屑粉晶灰岩，J21井，3408.10 m，太原组；（b）藻粘结灰岩，Q2井，2566.88 m，太原组；（c）生屑泥晶灰岩，M61井，2305.58 m，太原组；（d）生物体腔孔，Z4井，2364.4 m，太原组；（e）晶间孔及溶孔，T58井，3414.16 m，太原组；（f）裂缝有少量方解石充填S2井，2337 m，太原组。Figure 2. Limestone reservoir characteristics of the Taiyuan Formation in Ordos Basin(a) Biogenic crystal limestone, J21well, 3408.10 m, the Taiyuan Formation; (b) Algal cemented limestone, Q2 well, 2566.88 m, the Taiyuan Formation; (c) Bioclastic mudstone limestone, M61well,2305.58 m, the Taiyuan Formation; (d) Biological cavity, Z4well,2364.4 m, the Taiyuan Formation; (e) Intergranular and dissolved pores, T58 well, 3414.16 m, the Taiyuan Formation; (f) Fractures with small amount of calcite filling, S2 well,2337 m, the Taiyuan Formation.太原组地层根据沉积旋回、古生物、岩石学特征自下而上可划分为庙沟段、毛儿沟段、斜道段、东大窑段4个亚段。庙沟段位于8#煤、8#上煤之间，富含腕足类、蜓类化石，主要为一套深灰-灰黑色薄层（含）生物碎屑灰岩，分布范围小。毛儿沟段位于位于8#上煤、7#煤之间，中部常发育凝灰岩，富含腕足类、蜓类、珊瑚等化石，分布范围较广。斜道段位于7#煤、6#煤之间，富含腕足类、蜓类、珊瑚、海百合、苔藓虫等化石，为一套中—厚层的深灰色（含）生物碎屑灰岩，厚8~20 m，分布范围广。东大窑段位于6号煤之上，含小型腕足类、蜓类化石，主要为深灰色含生物碎屑灰岩，厚度2~10 m，分布范围小。受沉积压实、成岩胶结等作用的影响，太原组灰岩储层具有致密，孔喉小、非均质性强的特点，平均孔隙度2.1%，平均渗透率0.21 mD，平均喉道半径0.12 μm。储集空间主要有溶孔、晶间孔、裂缝（图2.d-f）。
2. 构造缝特征
2.1 盆地应力场特征
针对鄂尔多斯盆地应力场的研究，现在也基本形成了统一的认识:区域内主要受到印支期、燕山期、喜山期三期构造应力作用,每期应力场源动力、方向以及作用范围强弱不同[13−14]。
印支事件构造应力场构源于三叠纪末羌塘-华南板块在与华北板块的碰撞，华南板块的快速向北运动产生强大挤压力，导致了两陆块之间的地壳大规模缩短。华北板块处在华南板块与西伯利亚板块的挤压格局之中，产生了鄂尔多斯盆地的南北向挤压、东西向伸展的应力场。据张泓等学者的研究结果最大主压应力和最大剪切应力的高值域位于盆地的西半部，东部（含研究区）为低值域分布区。燕山运动的构造应力场与库拉—太平洋板块在晚侏罗世向 NW的俯冲有关。燕山运动在鄂尔多斯盆地的挤压构造应力为NW－SE向，构造应力场高值域主要分布于盆地的中南部（含研究区）。鄂尔多斯盆地喜马拉雅运动构造应力场的方向发生了根本的改变，即挤压方向由 NW 向转变为 NE，构造活动性主要集中于盆地的边缘地区。
区域内构造行迹展布特征与构造应力场演化有较好的一致性。区域构造应力场主要受到燕山运动的影响，燕山期构造应力场奠定了研究区的主要构造格架，以挤压应力为主，发育了NW-SE向挤压应力。
2.2 盆地构造单元划分
鄂尔多斯盆地自形成经历了太古-早元古代结晶基底形成阶段、中-晚元古代大陆裂解和碰撞造山阶段、早古生代隆坳相间构造格局形成阶段、晚古生代拉张沉降阶段以及中-新生代板块汇聚、碰撞造山阶段。其中，中-新生代板块汇聚及碰撞造山阶段的燕山运动和喜马拉雅运动决定了鄂尔多斯盆地南北翘起、东翼缓而长和西翼短而陡的现今构造格局，据此可将该盆地分为六大二级构造单元：伊盟隆起、晋西挠褶带、渭北隆起、西缘冲断带、天环坳陷和伊陕斜坡[15]。本文研究区位于伊陕斜坡二级构造单元的东北部，临近晋西挠褶带，为东高西低的单斜构造，斜坡较平缓，坡降每公里约3.9 m，地层倾角0.23°。受燕山期NW-SE应力场影响，研究区在单斜构造的背景上，发育一系列近于平行的NE-SW向小型的背斜、向斜、鼻隆（图3）构造，而灰岩脆性强，天然构造缝必然普遍发育。
图 3 研究区构造位置图与太原组灰岩顶面构造等值线图（a）构造位置图 （b）构造顶面位置图Figure 3. Structural location and top structure contour of the Taiyuan Formation in study area(a) Structural location map in study area; (b)Top structure contour map in study area2.3 构造缝发育特征
构造裂缝是指其分布、形态等受局部构造事件或构造应力场控制的裂缝[16−20]，裂缝的发育程度与发育特征随构造部位的不同而表现出明显差异[21−22]。研究区构造缝多见于纯的灰岩层中，在泥岩、泥质灰岩中构造缝不发育。根据岩心及野外剖面观察，构造缝主要包括剪切裂缝和张性裂缝，构造剪切缝形态较为规则，缝面平直光滑、产状分布稳定且多呈组出现（图4-a,b），缝宽分布较为均匀，岩心观察可见缝面上发育擦痕和微小陡坎(图4-c）。张性裂缝形态一般缝面粗糙，缝宽分布不均匀。按照裂缝的倾角可将构造裂缝进一步分为低角度缝(倾角≤30°)、斜交缝(倾角介于30°~60°)和高角度缝(倾角≥60°)。低角度缝常见于岩性有变化的界面，平面上分布最为广泛（图4-g），泥质、方解石半－全充填，充填程度性强，见压溶及缝合线构造，有效性差，但经高角度缝切割、错动后有效性变好。斜交缝常呈组出现，泥质、方解石未－半充填，充填程度性较弱、有效性较好。高角度缝延伸长度在0.3~9.0 m之间，野外缝延伸长度可超过10 m，甚至穿层，泥质、方解石未－半充填，常贯穿、切割、错动其它类型的裂缝，形成缝网系统，（图4-f，h），有效性好。从裂缝的有效性及储层物性改善方面考虑，高角度缝是最有利的裂缝类型。
图 4 太原组灰岩构造缝发育特征(a)共轭剪切缝，Q71井，太原组,2860.50 m；(b)共轭剪切缝，成家庄剖面；(c)剪切缝，裂面具阶步擦痕，SH137井，2478.24 m；(d)高角度缝，Q71，太原组，2860.50 m；(e)高角度缝，Q71井，太原组，2853.78 m；(f)网状缝，招贤剖面，2492.12 m；(g)水平缝，骆驼局剖面；(h)高角度缝水平缝相互切割，招贤剖面。Figure 4. Development characteristics of structural fractures in the Taiyuan limestone(a) Conjugate shear fractures, Q71 well, the Taiyuan Formation, 2860.50 m; (b) Conjugate shear fractures, Chengjiazhuang section; (c) Shear fractures, step scratches on crack surface, SH137 well, 2478.24 m; (d) High angle fractures, Q71 well, Taiyuan Formation, 2860.50 m; (e) High angle fractures, Q71 well, Taiyuan Formation, 2853.78 m; (f) fracture nets, Zhaoxian profile, 2492.12 m; (g) Horizontal fractures, Luotuoju section; (h) Mutual cutting of high angle fractures and horizontal fractures, Zhaoxian profile.2.4 构造缝产状
岩心观察及成像测井资料统计表明，太原组灰岩裂缝密度主要分布在0~15条/m之间，平均8条/m；裂缝宽度大部分小于0.5 mm，占59.3%；裂缝以方解石或泥质半－充填为主，半充填的占 40.1%。太原组灰岩裂缝倾角在59°~85°，平均69.3°，主要为高角度构造缝（表1）。裂缝方位在316°~345°，平均331.5°，经过与鄂尔多斯盆地构造应力场 [23]对比，表明太原组灰岩地层构造缝裂缝主要形成于燕山期。
表 1 太原灰岩典型井裂缝产状统计表Table 1. Statistics of typical well fracture occurrence in the Taiyuan limestone井号 SH108 M120 M130 M60 M120 M170 S122 M130 深度/m 2 403.0 2 555.5 1 646.3 2 555.7 1 645.4 2 243.3 2 206.6 2 310.7 倾角/° 85 61.0 68.3 60.9 72.4 73.5 74.3 59 方位角/° 341.5 340.2 324.6 345.0 320.6 329.0 335.1 316 3. 裂缝的成藏地质意义
3.1 控制了储层发育程度
生产中，面临着灰岩储层分析孔隙度与产气量不匹配的问题，以YT4H*井为例，储层段岩心分析孔隙度平均值为2.3%，试气产量却达到108.8万m3/d。分析实验表明灰岩储层整体上具有孔隙度小、喉道细、非均质性强的特点，绝大部分喉道半径小于2 μm（图5）。作为主要储集空间之一的晶间孔孔隙空间小，联通性差，但数量多（图6a），而生物溶孔孔隙空间相对较大，但普遍处于相互孤立的状态（图6b），裂缝的扩展，使得原本相对独立的孔隙空间联通性增强或相互沟通，构成了立体孔隙网络空间（图6c-f），提高致密灰岩的储集性能。构造缝对岩溶发育的控制已有较多研究[24−26]，而对于构造缝发育究竟能多大程度上改善致密灰岩储层物性缺少定量研究。核磁共振技术能够在不损伤岩石的情况下测得弛豫时间T2谱曲线和孔隙度[27−29]，为分析解决上述问题提供了一种可行的解决途径。研究采用单轴载荷下岩石核磁共振实验分析了裂缝扩展对不同岩性灰岩储层孔隙度的影响。
图 5 研究区太原组灰岩喉道半径分布频率图Figure 5. Frequency distribution of throat radius of the Taiyuan Formation limestone in study area
图 6 鄂尔多斯盆地太原组灰岩储层储集空间类型(a) 晶间孔发育，J21井，太原组，3413.09 m；(b) 相互孤立的生物体腔孔，G21井，太原组，2364.70 m，(c) 微裂联通接生物体腔壁溶孔，J21井，3413.10 m；(d) 溶孔、晶间孔、微裂缝，CT扫描俯视图，G21井，太原组，3404.13 m；(e) 溶孔、晶间孔、微裂缝，CT扫描侧视图，G21井，太原组，3404.13 m； (f) 孔隙空间立体网络，CT扫描透视图，G21井，太原组，3404.13 m。Figure 6. Reservoir space types of the Taiyuan Formation in Ordos Basin(a) Interstitial pore development, J21 well, the Taiyuan Formation, 3413.09 m; (b) Isolated biological cavities, G21 well, the Taiyuan Formation, 2364.70 m; (c) Microfracture connected to biological dissolution pore, J21 well, the Taiyuan Formation, 3413.10 m; (d) Dissolved pores, intergranular pores, microcracks, CT scan(top view) , G21 well, the Taiyuan Formation, 3404.13 m; (e) Dissolved pores, intergranular pores, microcracks, CT scan(side view), G21 well, the Taiyuan Formation, 3404.13 m; (f) Stereoscopic network of pore space, CT scan(perspective view), G21 well, the Taiyuan Formation, 3404.13 m.实验过程中分别选取代表性的储层岩性：生屑细粉晶灰岩，藻粘结灰岩，生屑泥晶灰岩，步骤如下:
（1） 将岩石样品加工成直径 2.5 cm，长度5 cm 的标准样品（图7）；
（2）对岩样进行洗油、洗盐、烘干；
（3）对岩石样品抽真空处理,然后充分饱和，用核磁共振仪测量岩样的T2衰减曲线,计算其静态孔隙度；
（4）在轴向对岩样缓慢施加载荷,然后用核磁共振仪测量岩样的T2衰减曲线，处理得到岩石样品T2谱分布,计算其动态孔隙度；
（5）对比分析不同样品裂缝扩展对储层物性的影响。
实验结果表明,岩石的核磁共振谱产生明显的变化，T2面积增大，谱峰整体右移（图8），总孔隙度增加。平均孔隙度由2.1%增加到4.2%,增加1倍。裂缝对总孔隙度的贡献率在14.3%~72.7%，平均值43.4%，3种储集岩性中，生屑粉晶灰岩孔隙度增加最大，平均为65.8%，藻粘结灰岩次之，平均为30.9%，生屑泥晶灰岩最小，平均为18.0%。泥晶灰岩、藻粘结灰岩、粉晶灰岩的基质孔隙依次增大，裂缝沟通的作用下，表现出粉晶灰岩孔隙度变化最大，藻粘结灰岩次之，泥晶灰岩相对最小（表2），因此构造缝的存在提升了太原组灰岩储层整体储集能力，提升程度因岩性不同各有差异。
图 8 M29井岩心实验前后核磁共振T2谱Figure 8. Core NMR T2 spectra before and afte rexperiment of M29 well表 2 太原灰岩静态、动态孔隙度对比表Table 2. Comparison of static and dynamic porosity of the Taiyuan Limestone样品号 井号 岩性 载荷/MPa 深度/m 核磁孔隙/% 孔隙度
增加量/%裂缝孔隙度
贡献率/%裂缝贡献率
平均值/%静态 动态 1 M29 生屑
粉晶
灰岩22.3 2 238.8 2.7 5.9 3.2 54.2 65.8 2 Y18 23.4 2 317.9 0.9 3.3 2.4 72.7 3 T59 28.4 3 412.4 1.9 6.9 5 72.5 4 M29 23.4 2 245.7 0.8 2.2 1.4 63.6 5 M120 藻粘结
灰岩23.4 2 549.2 1.7 2.3 0.6 26.1 30.9 6 Q3 23.6 2 718.8 1.8 2.4 0.6 25.0 7 M125 24.1 2 728.2 6.3 10.8 4.5 41.7 8 S5 生屑
泥晶
灰岩27.82 3 413.3 2 / / / 18.0 9 S2 22.8 2 339.9 1.2 1.4 0.2 14.3 10 Q2 24.7 2 568.8 1.8 2.3 0.5 21.7 3.2 形成了有效的输导系统
在野外剖面与三维地震解释资料上均可见到明显的缝网系统。野外剖面上，高角度裂缝开启度高、沟通性强，纵向上切割水平成岩缝，大大增加了输导的有效性与广泛性（图9）。三维地震解释资料亦可见裂缝相互切割，形成发育的缝网系统（图10）。流体包裹体作为古地质流体原始信息的有效赋存体，成为研究油气流体示踪的重要手段[30−33]。太原组灰岩储层裂缝的方解石脉中常见黄色荧光（图11-a，b），在显微激光拉曼光谱图中有明显的沥青及甲烷拉曼散射峰特征。沥青包裹体在偏光显微镜下呈黑色，不透明，形态多呈不规则状，在扫描光谱图中，沥青质拉曼散射峰在
1573 ~1613 cm−1（图11-c、d）。甲烷包裹体主要分布比较粗大透明的方解石颗粒中，形态为圆形、椭圆形。在扫描光谱图中，甲烷拉曼散射峰在2914 cm−1（图11-e、f）。灰岩储层流体包裹体均一温度呈单峰状分布，具有连续充注成藏的特征，峰值集中于120 ℃~160 ℃（图12）。参考工区典型井成藏温度、埋藏史、热演化史[34]，可确定广泛发育的缝网形成了有效的输导系统，在主成藏期晚侏罗世－早白垩世烃类通过缝网系统进行了有效的运移（图13）。灰岩储层夹于主力煤系烃源岩8#煤、5#煤之间，且与8#上煤、7#煤、6#煤等多套薄煤层、碳质泥岩直接接触，加之灰岩自身亦具备一定的生烃能力，烃源岩生成的天然气通过断裂系统进入灰岩储层聚集，辅以太原组顶部海相泥岩的直接盖层，形成“三明治”结构岩性气藏。
图 9 缝网系统贯穿烃源岩与灰岩储集体（成家庄剖面）Figure 9. Source rock and limestone reservoir are connected by fracture nets (Chengjiazhuang section)
图 10 鄂尔多斯盆地东部太原组灰岩断裂系统平面图(地震解释，主要反映高角度缝)Figure 10. Fault-fracture System of Taiyuan Limestone in the Eastern Ordos Basin (Seismic Interpretation, mainly reflecting high angle fractures)
图 11 盆地太原组灰岩裂缝中甲烷包裹体、沥青包裹体产状形态特征及激光拉曼光谱(a) 构造缝，方解石充填，单偏光5倍，T65井，3 247.29 m；(b) 方解石脉体荧光显示，发黄色光，T65井，3 247.29 m；(c) 单个沥青质包裹体，T65井，3 247.29 m；(d)单个沥青质包裹体激光拉曼光谱，T65井，3 247.29 m；(e)单个甲烷包裹体，Q2井，2 564.01 m；(f) 单个甲烷包裹体激光拉曼光谱，Q2井，2 564.01 m。Figure 11. Occurrence morphology and laser Raman spectroscopy characteristics of methane and asphalt inclusions in the fractures of the Taiyuan limestone in the basin(a) structural fracture, filled with calcite, 5x single polarization, T65 well, 3 247.29 m; (b) Calcite vein fluorescence , yellow light, T65 well, 3 247.29 m; (c) Single asphaltene inclusion, T65 well, 3 247.29 m; (d) Laser Raman spectroscopy of single asphaltene inclusion, T65 well, 3 247.29 m; (e) Single methane inclusion, Q2 well, 2 564.01 m; (f) Laser Raman spectroscopy of single methane inclusion , Q2 well, 2 564.01 m
图 12 盆地太原组灰岩储层裂缝流体包裹体均一温度分布频率图Figure 12. Uniform temperature distribution frequency map of fluid inclusions in fractures of Taiyuan limestone reservoir in the basin
图 13 鄂尔多斯盆地陕参1井热演化史图（据任战利）Figure 13. Thermal evolution history of Shancan-1 well in Ordos Basin (by Ren Zhanli)4. 构造缝的预测
裂缝预测方法主要有测井、地震信息裂缝预测法、构造应力场数值模拟法、主控因素法[35−39]。测井、地震信息裂缝预测法预测结果可靠性高，是目前最主要的裂缝预测技术，但是研究区三维地震资料、成像测井资料有限。构造应力场数值模拟技术近几年逐渐发展完善，由于构造演化的复杂性，该技术在区域裂缝发育情况方面可以提供相对较为准确的信息，但具体到单井上的准确性依旧有待提高[40]。主控因素一般包括构造位置和岩性，构造位置又可以进一步划分为褶皱和断层。根据褶皱与裂缝相关性对裂缝预测的方法即为经典的曲率法[41]，在研究区，褶皱、鼻隆构造发育，且岩地层脆性矿物含量高，综合考虑后采用曲率法预测构造缝。曲率可以反映地质体的弯曲程度，当地层受构造应力挤压时，会沿发生弯曲变形，变形越剧烈（即曲率越大），断裂越发育。研究区灰岩地层分布稳定，储层主要位于地层中上部（图14），为进一步分辨本次研究关心高角度张性裂缝的发育区，研究对经典的高斯曲率法做了改造，构建改进的高斯曲率法（IGC）预测有利构造缝的发育区。
假设脆性地层出示状态为水平，当受构造应力挤压时，会弯曲变形，地层上隆部位承受拉张应力而形成张裂缝（储层主要在地层中上部），下凹陷地层则承受挤压，容易产挤压缝、缝合线等，上隆与下凹之间的的地层因相对滑动，容易产生剪切缝、劈理（图15）。相同构造应力作用下，粉晶灰岩（泥质含量小，脆性强）最易产生裂缝，藻粘结灰岩、泥晶灰岩次之。上隆部位一方面处于构造高点，易于天然气聚集成藏，另一方面，张裂缝发育，利于储层发育，是天然气勘探的首选地质目标。下凹部位处于构造低点，易于产水，建议谨慎部署井位。
图 15 地层弯曲变形与裂缝性质简图Figure 15. Schematic diagram of geological deformation and fracture properties对于一个地层面，假定其构造变形复杂，最大曲率Cmax与最小曲率Cmin均不等于0，即：Cmax、Cmin≠0。
定义方向系数δ：
If Cmax&&Cmin>0,δ=1
else δ=−1
end
改进的高斯曲率值即为：
IGC=δ*Cmin*Cmax
地质意义：
IGC>0时，地质体为正地形，|IGC|↑，高角度张性裂缝越发育；
IGC<0时，地质体为负地形，|IGC|↑，挤压缝越发育；
IGC≈0时，地质体变形弱，主要发育剪切缝、劈理。
因此： IGC>0&&|IGC|↑时，地质目标↑有利。
5. 应 用
该方法首先在横山地区进行了应用，对井位部署进行了支撑。具体步骤如下：步骤1，准备并检查工区构造数据集；步骤2，根据所述步骤1的构造数据拟合构造面；步骤3，计算拟合构造面的的最大曲率Cmax，最小曲率Cmin以及方向因子δ；步骤4，计算评价参数IGC；步骤5，绘制评价参数IGC平面等值线图，结合地质背景确定有利勘探地质目标。S476，S180、S159等红色区域为Ⅰ类有利区，高角度张性裂缝最发育，综合考虑其它成藏地质因素以及现场实施情况，在S476井场部署了YT1H井。后期的成像测井解释表明该井储层段高角度缝发育（图16），倾角主要在75。-90。（图17），试气产量达到54万m3/d，实现了盆地太原组灰岩勘探突破。近2年来在，陆续在Ⅰ类有利区S476，T53发现发现工业气流井9口， 10万方以上5口，YT3H*，获无阻流量63.0万m3/d，YT4H*，获无阻流量108.8万m3/天（图18）。
图 16 YT1H井太原组测井综合解释成果蓝图Figure 16. Logging Comprehensive Interpretation Results of YT1H Well in Taiyuan Formation
图 18 横山北地区太原组灰岩勘探成果图Figure 18. Exploration achievement of the Taiyuan limestone in Northern Hengshan6. 结论与建议
6.1 结 论
(1)按照裂缝的倾角可将构造裂缝进分为低角度缝、斜交缝和高角度缝。这3种基本类型中高角度构造张裂缝充填程度低，有效性最好，常贯穿、切割、错动其它类型的裂缝形成缝网系统。
（2）裂缝对致密灰岩储层物性有极大贡献作用，也是有效的输导系统。平均孔隙度由2.1%增加到4.2%,增加1倍，裂缝对总孔隙度的贡献率在14.3%~72.7%，平均值43.4%。5#煤、8#煤等烃源岩生成的天然气通过缝网系统有效输导进入灰岩储层聚集，形成“三明治”结构岩性气藏。
（3）改进的高斯曲率法（IGC）可预测有利构造缝的发育区，IGC值越大，高角度张性裂缝越发育，勘探目标越有利。
6.2 建 议
（1）理论上，加强构造缝，尤其是高角度构造缝的理论模型研究，推导三维空间下鼻隆体构造缝的理论孔隙度、渗透率计算公式，使研究由定性向定量转变。（2）空间上，寻找缝网、有利岩性、主力烃源岩及盖层的叠合区，预测气藏甜点区，指导勘探开发。
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图 1 鄂尔多斯盆地太原组灰岩分布与地层特征
（a）地层特征 （b）灰岩平面分布
Figure 1. Distribution and stratigraphy characteristics of the Taiyuan Formation limestone in Ordos Basin
(a)Stratigraphy characteristics;(b)Thicknes distribution of Taiyuan limestone
图 2 鄂尔多斯盆地太原组灰岩储层特征
（a）生屑粉晶灰岩，J21井，3408.10 m，太原组；（b）藻粘结灰岩，Q2井，2566.88 m，太原组；（c）生屑泥晶灰岩，M61井，2305.58 m，太原组；（d）生物体腔孔，Z4井，2364.4 m，太原组；（e）晶间孔及溶孔，T58井，3414.16 m，太原组；（f）裂缝有少量方解石充填S2井，2337 m，太原组。
Figure 2. Limestone reservoir characteristics of the Taiyuan Formation in Ordos Basin
(a) Biogenic crystal limestone, J21well, 3408.10 m, the Taiyuan Formation; (b) Algal cemented limestone, Q2 well, 2566.88 m, the Taiyuan Formation; (c) Bioclastic mudstone limestone, M61well,2305.58 m, the Taiyuan Formation; (d) Biological cavity, Z4well,2364.4 m, the Taiyuan Formation; (e) Intergranular and dissolved pores, T58 well, 3414.16 m, the Taiyuan Formation; (f) Fractures with small amount of calcite filling, S2 well,2337 m, the Taiyuan Formation.
图 3 研究区构造位置图与太原组灰岩顶面构造等值线图
（a）构造位置图 （b）构造顶面位置图
Figure 3. Structural location and top structure contour of the Taiyuan Formation in study area
(a) Structural location map in study area; (b)Top structure contour map in study area
图 4 太原组灰岩构造缝发育特征
(a)共轭剪切缝，Q71井，太原组,2860.50 m；(b)共轭剪切缝，成家庄剖面；(c)剪切缝，裂面具阶步擦痕，SH137井，2478.24 m；(d)高角度缝，Q71，太原组，2860.50 m；(e)高角度缝，Q71井，太原组，2853.78 m；(f)网状缝，招贤剖面，2492.12 m；(g)水平缝，骆驼局剖面；(h)高角度缝水平缝相互切割，招贤剖面。
Figure 4. Development characteristics of structural fractures in the Taiyuan limestone
(a) Conjugate shear fractures, Q71 well, the Taiyuan Formation, 2860.50 m; (b) Conjugate shear fractures, Chengjiazhuang section; (c) Shear fractures, step scratches on crack surface, SH137 well, 2478.24 m; (d) High angle fractures, Q71 well, Taiyuan Formation, 2860.50 m; (e) High angle fractures, Q71 well, Taiyuan Formation, 2853.78 m; (f) fracture nets, Zhaoxian profile, 2492.12 m; (g) Horizontal fractures, Luotuoju section; (h) Mutual cutting of high angle fractures and horizontal fractures, Zhaoxian profile.
图 5 研究区太原组灰岩喉道半径分布频率图
Figure 5. Frequency distribution of throat radius of the Taiyuan Formation limestone in study area
图 6 鄂尔多斯盆地太原组灰岩储层储集空间类型
(a) 晶间孔发育，J21井，太原组，3413.09 m；(b) 相互孤立的生物体腔孔，G21井，太原组，2364.70 m，(c) 微裂联通接生物体腔壁溶孔，J21井，3413.10 m；(d) 溶孔、晶间孔、微裂缝，CT扫描俯视图，G21井，太原组，3404.13 m；(e) 溶孔、晶间孔、微裂缝，CT扫描侧视图，G21井，太原组，3404.13 m； (f) 孔隙空间立体网络，CT扫描透视图，G21井，太原组，3404.13 m。
Figure 6. Reservoir space types of the Taiyuan Formation in Ordos Basin
(a) Interstitial pore development, J21 well, the Taiyuan Formation, 3413.09 m; (b) Isolated biological cavities, G21 well, the Taiyuan Formation, 2364.70 m; (c) Microfracture connected to biological dissolution pore, J21 well, the Taiyuan Formation, 3413.10 m; (d) Dissolved pores, intergranular pores, microcracks, CT scan(top view) , G21 well, the Taiyuan Formation, 3404.13 m; (e) Dissolved pores, intergranular pores, microcracks, CT scan(side view), G21 well, the Taiyuan Formation, 3404.13 m; (f) Stereoscopic network of pore space, CT scan(perspective view), G21 well, the Taiyuan Formation, 3404.13 m.
图 8 M29井岩心实验前后核磁共振T2谱
Figure 8. Core NMR T2 spectra before and afte rexperiment of M29 well
图 9 缝网系统贯穿烃源岩与灰岩储集体（成家庄剖面）
Figure 9. Source rock and limestone reservoir are connected by fracture nets (Chengjiazhuang section)
图 10 鄂尔多斯盆地东部太原组灰岩断裂系统平面图(地震解释，主要反映高角度缝)
Figure 10. Fault-fracture System of Taiyuan Limestone in the Eastern Ordos Basin (Seismic Interpretation, mainly reflecting high angle fractures)
图 11 盆地太原组灰岩裂缝中甲烷包裹体、沥青包裹体产状形态特征及激光拉曼光谱
(a) 构造缝，方解石充填，单偏光5倍，T65井，3 247.29 m；(b) 方解石脉体荧光显示，发黄色光，T65井，3 247.29 m；(c) 单个沥青质包裹体，T65井，3 247.29 m；(d)单个沥青质包裹体激光拉曼光谱，T65井，3 247.29 m；(e)单个甲烷包裹体，Q2井，2 564.01 m；(f) 单个甲烷包裹体激光拉曼光谱，Q2井，2 564.01 m。
Figure 11. Occurrence morphology and laser Raman spectroscopy characteristics of methane and asphalt inclusions in the fractures of the Taiyuan limestone in the basin
(a) structural fracture, filled with calcite, 5x single polarization, T65 well, 3 247.29 m; (b) Calcite vein fluorescence , yellow light, T65 well, 3 247.29 m; (c) Single asphaltene inclusion, T65 well, 3 247.29 m; (d) Laser Raman spectroscopy of single asphaltene inclusion, T65 well, 3 247.29 m; (e) Single methane inclusion, Q2 well, 2 564.01 m; (f) Laser Raman spectroscopy of single methane inclusion , Q2 well, 2 564.01 m
图 12 盆地太原组灰岩储层裂缝流体包裹体均一温度分布频率图
Figure 12. Uniform temperature distribution frequency map of fluid inclusions in fractures of Taiyuan limestone reservoir in the basin
图 13 鄂尔多斯盆地陕参1井热演化史图（据任战利）
Figure 13. Thermal evolution history of Shancan-1 well in Ordos Basin (by Ren Zhanli)
图 15 地层弯曲变形与裂缝性质简图
Figure 15. Schematic diagram of geological deformation and fracture properties
图 16 YT1H井太原组测井综合解释成果蓝图
Figure 16. Logging Comprehensive Interpretation Results of YT1H Well in Taiyuan Formation
图 18 横山北地区太原组灰岩勘探成果图
Figure 18. Exploration achievement of the Taiyuan limestone in Northern Hengshan
表 1 太原灰岩典型井裂缝产状统计表
Table 1. Statistics of typical well fracture occurrence in the Taiyuan limestone
井号 SH108 M120 M130 M60 M120 M170 S122 M130 深度/m 2 403.0 2 555.5 1 646.3 2 555.7 1 645.4 2 243.3 2 206.6 2 310.7 倾角/° 85 61.0 68.3 60.9 72.4 73.5 74.3 59 方位角/° 341.5 340.2 324.6 345.0 320.6 329.0 335.1 316 
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表 2 太原灰岩静态、动态孔隙度对比表
Table 2. Comparison of static and dynamic porosity of the Taiyuan Limestone
样品号 井号 岩性 载荷/MPa 深度/m 核磁孔隙/% 孔隙度
增加量/%裂缝孔隙度
贡献率/%裂缝贡献率
平均值/%静态 动态 1 M29 生屑
粉晶
灰岩22.3 2 238.8 2.7 5.9 3.2 54.2 65.8 2 Y18 23.4 2 317.9 0.9 3.3 2.4 72.7 3 T59 28.4 3 412.4 1.9 6.9 5 72.5 4 M29 23.4 2 245.7 0.8 2.2 1.4 63.6 5 M120 藻粘结
灰岩23.4 2 549.2 1.7 2.3 0.6 26.1 30.9 6 Q3 23.6 2 718.8 1.8 2.4 0.6 25.0 7 M125 24.1 2 728.2 6.3 10.8 4.5 41.7 8 S5 生屑
泥晶
灰岩27.82 3 413.3 2 / / / 18.0 9 S2 22.8 2 339.9 1.2 1.4 0.2 14.3 10 Q2 24.7 2 568.8 1.8 2.3 0.5 21.7
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