Paleo-Fluid Migration and Conservation Conditions of Shale Gas in Jiaoshiba-Wulong Area
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摘要: 焦石坝-武隆地区差异构造带发育，古流体活动复杂，对页岩气保存条件影响较为关键.以两类典型背斜（高陡背斜和箱状背斜）的裂缝脉为研究对象，基于裂缝分形理论和碳、氧、锶同位素地球化学理论，揭示出不同构造的古流体活动差异与页岩气保存条件优劣的耦合性.研究认为：（1）构造变形与古流体活动性存在耦合性.构造应力集中部位（如箱状背斜枢纽、隐伏断层）较构造其他部位具更强的流体活动性.（2）古流体示踪差异与页岩气保存条件存在耦合性.同位素地球化学揭示出二叠系-下三叠统以内源流体活动为主，封闭能力较好，盆内高陡背斜带和盆外残余向斜五峰-龙马溪组页岩气具备一定勘探前景；中寒武统-下奥陶统存在跨层流体活动的痕迹，封闭能力变差，盆外箱状背斜下寒武统筇竹寺组页岩气勘探风险加大.Abstract: The development of the differential tectonic zones in the Jiaoshiba-Wulong area with complex paleo-fluid activities is crucial to the preservation of shale gas. The fracture veins of two typical anticlines (steep anticlines and box anticlines) are studied. Based on the theory of fractal fracture and carbon, oxygen and strontium isotope geochemistry, it reveals the differences of paleo-fluid activities in different structure and coupling of shale gas preservation conditions. The study suggests fellows:(1) There is coupling between tectonic deformation and paleo-fluid activity. The fluid is more active in the tectonic stress concentration areas (such as box anticlinal hinge, hidden faults) than other parts of the structure. (2) There is coupling between paleo-fluid tracer differences and shale gas preservation conditions. Isotope geochemistry reveals that the internal fluid flow dominates in the Permian-Lower Triassic formation, and the sealing ability is good. The Wufeng-Longmaxi shale gas of the high-steep anticline in the basin and the residual syncline outside the basin has certain exploration prospects. There exists the trace of cross-layer fluid activities in the Middle Cambrian-Lower Ordovician formation, and the sealing ability deteriorates. The risks of shale gas exploration in the Lower Cambrian Qiongzhusi Formation of the box anticline outside the basin increased.
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Key words:
- Sichuan basin /
- fracture fractal /
- carbon, oxygen and strontium isotope /
- paleo-fluid /
- shale gas
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图 1 四川盆地川东南地区地质简图(a)及实测构造剖面图(b)
Fig. 1. Geological map (a) and measured structural section (b) of the southeastern area in Sichuan basin
图 2 焦石坝-大耳山地区典型脉体及裂缝分形学构造剖面
B201井为投影位置,黄色实线表示地层,红色虚线表示裂缝脉
Fig. 2. Typical vein and fracture fractal section in the Jiaoshiba-Daershan area
图 3 接龙场背斜典型脉体及裂缝分形学构造剖面
黄色实线表示地层，红色虚线表示裂缝脉
Fig. 3. Typical vein and fracture fractal section in Jielongchang anticline
图 4 焦石坝-大耳山构造脉体的锶同位素特征
Fig. 4. Graph of strontium isotope of the veins in the Jiaoshiba-Daershan structure
图 5 接龙场背斜脉体的锶同位素特征
Fig. 5. Graph of strontium isotope of veins in the Jielongchang anticline
表 1 焦石坝-武隆地区裂缝特征统计
Table 1. tatistical data of fracture features in the Jiaoshiba-Wulong area
构造名称 采样点 层位 地层产状(°) 均脉宽(mm) 脉密度(条/m) 脉宽密度(mm/m) 变差系数Cv 分维数D 拟合度R2 焦石坝
背斜东部10* 嘉陵江组T1j 78∠8 2.39 18 44 1.000 1.64 0.96 25* 嘉陵江组T1j 90∠6 1.98 13 25 1.340 1.75 0.94 大耳山
高陡
背斜18* 嘉陵江组T1j 125∠76 1.72 39 68 1.160 1.71 0.98 15 上二叠统P2 104∠70 1.65 34 56 0.780 2.53 0.90 14 上二叠统P2 103∠68 1.57 39 62 0.995 2.11 0.97 9 下二叠统P1 93∠40 1.35 61 84 0.620 2.49 0.98 7※ 上二叠统P2 95∠53 1.46 38 57 1.060 2.16 0.99 5※ 飞仙关组T1f 115∠58 2.63 21 56 0.810 1.53 0.97 2 嘉陵江组T1j 36∠28 2.05 23 48 0.910 2.10 0.85 38 嘉陵江组T1j 116∠23 1.20 32 38 0.700 2.38 0.93 接龙场
箱状
背斜590 飞仙关组T1f 315∠24 1.38 15 22 1.319 2.08 0.99 592 上二叠统P2 292∠54 4.33 25 111 0.625 1.08 0.96 593 下二叠统P1 240∠73 5.55 18 184 1.257 0.80 0.98 599 大湾组O1d 333∠19 2.55 12 30 1.066 1.28 0.99 600 后坝组 C3h38∠11 1.98 11 22 1.154 1.82 0.94 602 平井组 C2p38∠11 1.79 33 61 1.120 1.64 0.98 607 桐梓组O1t 291∠24 1.85 45 84 1.000 1.49 0.97 611 平井组 C2p73∠12 1.84 19 36 0.582 1.13 0.89 612 平井组 C2p97∠13 2.16 16 36 1.326 1.88 0.96 616 平井组 C2p285∠76 2.02 34 71 0.647 1.61 0.98 627 上二叠统P2 110∠25 1.87 25 47 1.127 1.44 0.93 注：采样点中带*标注(如10*)位于大耳山西隐伏断层附近；带※标注(如7※)位于大耳山东侧隐伏断层附近. 
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表 2 焦石坝-武隆地区裂缝脉及围岩的碳氧锶同位素
Table 2. Carbon, oxygen and strontium isotope data of fracture vein and country rock in the Jiaoshiba-Wulong area
样品号 地层 围岩(c) 裂缝脉(v) 围岩-裂缝脉(c-v) 描述 (87Sr/86Sr)(c) δ13C(c)
(‰)δ18O(c)
(‰)描述 (87Sr/86Sr)(v) δ13C(v)
(‰)δ18O(v)
(‰)Δ(87Sr/86Sr)(c-v)
(10-4)Δδ13C(c-v)
(‰)Δδ18O(c-v)
(‰)10-1S T1j 生物屑灰岩 0.708 03 -1.9 23.8 张性方解石脉 0.707 85 -2.3 24.9 1.8 0.4 -1.1 10-2S T1j 生物屑灰岩 0.708 03 -1.9 23.8 破碎带内粗晶
方解石脉0.707 61 -2.1 23.9 4.2 0.2 -0.1 25S T1j 泥晶灰岩 0.708 12 -1.4 23.4 节理方解石脉 0.707 86 -2.4 24.1 2.6 1.0 -0.7 18S T1j 泥晶灰岩 0.708 04 1.0 22.6 节理方解石脉 0.707 99 -1.1 20.4 0.5 2.1 2.2 15S P2 瘤状灰岩 0.707 29 2.1 44.3 张性方解石脉 0.707 28 1.6 23.5 0.1 0.5 20.8 14S P2 泥晶灰岩 0.707 18 3.6 24.9 剪张性方解石脉 0.707 21 1.0 23.1 -0.3 2.6 1.8 9S P1 泥晶灰岩 0.707 55 4.3 22.8 剪张性方解石脉 0.707 32 3.5 21.5 2.3 0.8 1.3 7S P2 生物屑灰岩 0.707 26 4.8 24.7 节理方解石脉 0.707 44 2.7 21.9 -1.8 2.1 2.8 5S T1f 砂屑灰岩 0.707 92 -1.3 22.6 张性方解石脉 0.707 90 -1.8 15.4 0.2 0.5 7.2 2S T1j 泥晶灰岩 0.708 59 -0.5 24.9 节理方解石脉 0.708 21 -2.4 17.7 3.8 1.9 7.2 38S T1j 泥晶灰岩 0.708 06 3.2 25.7 方解石脉 0.708 05 -2.4 18.4 0.1 5.6 7.3 590S T1f 粒屑灰岩 0.707 45 2.5 22.9 张节理方解石脉 0.707 33 1.3 22.8 1.2 1.2 0.1 592S P2 泥晶灰岩 0.707 41 2.7 23.6 张性方解石脉 0.707 54 1.4 22.5 -1.3 1.3 1.1 593-1S P1 瘤状灰岩 0.707 23 4.1 22.6 剪张性方解石脉 0.707 73 2.2 21.6 -5.0 1.9 1.1 593-2S P1 瘤状灰岩 0.707 23 4.1 22.6 张性方解石脉 0.708 11 1.9 21.5 -8.8 2.2 1.1 593-3S P1 瘤状灰岩 0.707 23 4.1 22.6 方解石脉 0.707 73 2.9 21.5 -5.0 1.2 1.1 597S S1ln 粉砂岩 0.730 76 \ \ 石英 0.717 46 \ \ 133.0 \ \ 599S O1d 生物屑灰岩 0.715 25 -0.5 19.5 剪张性方解石脉 0.723 34 -1.9 18.6 -80.9 1.4 0.9 600S C3h砂屑白云岩 0.711 09 2.0 22.5 张性方解石脉 0.709 66 -2.0 13.0 14.3 4.0 9.5 602S C2p泥质白云岩 0.710 17 0.1 22.7 顺层方解石脉 0.709 16 -1.2 20.2 10.1 1.3 2.5 607S O1t 泥晶灰岩 0.709 17 -2.5 21.7 张性方解石脉 0.709 59 -3.3 19.0 -4.2 0.8 2.7 611-1S C2p泥晶灰岩 0.709 17 -2.5 21.7 晶洞方解石脉 0.710 18 -7.8 19.0 -10.1 5.3 2.7 611-2S C2p颗粒灰岩 0.709 62 -1.3 22.3 节理方解石脉 0.710 38 -1.0 21.5 -7.6 -0.3 0.8 612S C2p砂屑白云岩 0.708 36 -1.1 22.1 剪张性方解石脉 0.709 59 -3.1 19.1 -12.3 2.0 3.0 616S C2p泥晶白云岩 0.709 71 -0.8 23.5 张性方解石脉 0.709 28 -1.1 20.3 4.3 0.3 3.2 627S P2 生物灰岩 0.707 09 4.2 24.5 张性方解石脉 0.707 05 1.7 25.1 0.4 2.5 -0.6 630S T1j 泥晶白云岩 0.709 52 -0.7 23.1 张性方解石脉 0.707 58 -1.0 19.2 19.4 0.3 3.9 注:(1)δ13C采用PDB标准, δ18O采用SMOW标准; (2)地质历史时期正常海水87Sr/86Sr值范围, T1:0.707 4~0.708 5;P2:0.706 7~0.707 6; P1:0.707 3~0.708 3;S1:0.707 8~0.708 7;O2-3:0.707 9~0.708 8;O1:0.708 8~0.709 3; C2-3:0.708 1~0.709 3;(3)15S的δ18O(c)异常高，不做讨论.
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