Stratigraphic characteristics and shale gas enrichment interval distribution of the Lower Cambrian Qiongzhusi Formation, Upper Yangtze region, China
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摘要:目的
上扬子地区下寒武统筇竹寺组页岩不仅保留重要的原始沉积海洋信息，更是重要的烃源岩和储集层，已展示出巨大的页岩气勘探潜力。
方法基于地震、钻井和露头资料，通过系统地层划分和对比，开展页岩地层和分布，明确页岩气甜点段。
结果和结论结果表明：上扬子地区下寒武统筇竹寺组划分为，筇一段(筇一1至筇一4亚段)和筇二段(筇二1至筇二4亚段)。(2) 麦地坪组和筇一段主要发育于德阳—安岳克拉通内裂陷内，而筇二段在裂陷外亦有广泛分布。裂陷内部地层结构表现为麦地坪组至筇一段东西两侧终止于灯影组灰岩，西侧厚度变化较缓，东侧地层快速尖灭；南北方向上，筇一段由北向南减薄，筇二段中部薄而南北厚。裂陷外部则以筇二段全区发育为特征，其中筇二1亚段直接超覆于筇一段或灯影组灰岩之上。(3) 筇二1亚段页岩具有优越的生烃、储集以及垂向和侧向封堵条件，为页岩气的富集段。内裂陷北段天星1井筇二1亚段页岩微孔隙和微裂缝发育，测井孔隙率为4.93%~6.57%，平均5.08%；德阳—安岳克拉通内裂陷槽中部的威页1井筇竹寺组筇二1亚段页岩有机质孔发育，测井孔隙率为4.20%~4.70%，平均4.51%；内裂陷南部的云南曲靖地区钻井井位有曲页1井、曲地1井等，筇竹寺组黑色页岩孔隙发育，高压压汞孔隙率为1.59%~11.33%，平均5.0%。(4)相比之下，尽管筇一段页岩在生烃和储集条件上表现良好，但其生成的页岩气易侧向沿岩溶带或断层逸散，不利于原地聚集成藏。如，内裂陷北段的川深1井，筇一3亚段厚约40 m，测井TOC含量平均3.5%，测井孔隙率平均6.4%，均为优质烃源岩和储集层，不利于原位聚集成藏。综上，筇二1亚段页岩因其高孔隙率和良好的封堵条件，为页岩气勘探的“甜点段”，为下一步油气勘探提供依据和指导。
Abstract:ObjectiveShales in the Lower Cambrian Qiongzhusi Formation within the Upper Yangtze region preserve critical information about primitive oceans. Furthermore, these shales serve as vital source rocks and reservoirs, having demonstrated considerable potential for shale gas exploration.
MethodsUsing seismic, borehole, and outcrop data, this study investigated the shale strata and their distribution in the Qiongzhusi Formation through comparative analysis. Accordingly, the sweet-spot interval was determined.
Results and conclusionsThe results indicate that the Lower Cambrian Qiongzhusi Formation in the Upper Yangtze region can be divided into the first and second members (also referred to as the Qiong 1 and 2 members, respectively), with the former consisting of Q1-1 to Q1-4 sub-members and the latter comprising Q2-1 to Q2-4 sub-members. The Maidiping Formation and the Qiong 1 Member predominantly occur within the Deyang-Anyue intracratonic rift, while the Qiong 2 Member is extensively distributed both inside and outside the rift. Within the rift, the west and east sides of the Maidiping Formation - Qiong 1 Member terminates at the limestone of the Dengying Formation, with the west side gradually thinning while the east side pinching out rapidly. In the north-south direction, the Qiong 1 Member thins southward, while the Qiong 2 Member is thin in the central part but thick in the northern and southern parts. Outside the rift, the Qiong 2 Member is distributed throughout the region, with the Q2-1 sub-member directly overlapping either the Qiong 1 Member or the limestone of the Dengying Formation. Shales in the Q2-1 sub-member enjoy superior hydrocarbon generation and reservoir conditions, as well as vertical/lateral sealing performance, emerging as a shale gas enrichment interval. For instance, in the northern part of the intracratonic rift, shales in the Q2-1 sub-member in well Tianxing-1 contain well-developed micropores and microfractures, with logging-derived porosity ranging from 4.93% to 6.57% (average: 5.08%). In the central part of the Deyang-Anyue intracratonic rift trough, shales in the Q2-1 sub-member in well Weiye-1 well exhibit organic matter-hosted pores, with logging-derived porosity ranging from 4.20% to 4.70% (average: 4.51%). In the Qujing area, Yunnan Province, within the southern part of the rift, black shales in the Qiongzhusi Formation in wells Qudi-1 and Quye-1 reveal well-developed black shales with high-pressure mercury injection-derived porosity spanning 1.59% to 11.33% (average: 5.0%). Although shales in the Qiong 1 Member exhibit favorable source-reservoir properties, the shale gas generated is prone to escape along karst zones or faults, unconducive to in-situ accumulation. For instance, in the northern part of the intracratonic rift, the Q1-3 submember in well Chuanshen-1 exhibits a thickness of about 40 m, logging-derived average TOC of 3.5%, and logging-derived porosity of 6.4%, suggesting high-quality source rocks and reservoirs but unfavorable conditions for in-situ accumulation. Overall, shales in the Q2-1 sub-member are identified as a sweet-spot interval for shale gas exploration due to their high porosity and great sealing performance. This study can serve as a critical basis and guide for future shale gas exploration in the Upper Yangtze region.
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图 1 上扬子地区地质及沉积概况
(a) 早寒武世华南板块位置[40]；(b) 上扬子地区早寒武世古地貌及研究点分布；(c) 上扬子地区前寒武纪—寒武纪地层综合柱状图
Fig. 1 Geological and sedimentary overview of the Upper Yangtze region
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图 2 上扬子地区下寒武统麦地坪组—筇竹寺组地层综合柱状图
注：Seqm1为层序代码；MFS为最大海泛面；TST为海侵体系域；HST为高位体系域。
Fig. 2 Composite stratigraphic column of the Lower Cambrian Maidiping and Qiongzhusi formations, Upper Yangtze region
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图 3 上扬子地区下寒武统麦地坪组—筇竹寺组二维地震剖面
Fig. 3 2D seismic profiles of the Lower Cambrian Maidiping and Qiongzhusi formations, Upper Yangtze region
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图 4 大薄片照片展示上扬子地区威207井下寒武统麦地坪组—筇竹寺组不同层段页岩沉积构造特征
(a) 小型交错层理，3 018.84 m，筇二2亚段；(b) 波状交错层理，3 056.54 m，筇二1亚段；(c) 书页状水平层理，3 146.60 m，筇一4亚段；(d) 书页状水平层理，3 236.23 m，筇一1亚段
Fig. 4 Photomicrographs of large thin sections showing the sedimentary texture characteristics of shales in the Lower Cambrian Maidiping and Qiongzhusi formations in well Wei 207 in the Upper Yangtze region
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图 5 上扬子地区垂直裂陷方向下寒武统麦地坪组—筇竹寺组连井地层对比剖面
Fig. 5 Well-correlation section of the Lower Cambrian Maidiping and Qiongzhusi formations perpendicular to the rift direction in the Upper Yangtze region
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图 6 上扬子地区平行裂陷方向下寒武统麦地坪组—筇竹寺组地层展布
Fig. 6 Stratigraphic distribution of the Lower Cambrian Maidiping and Qiongzhusi formations parallel to the rift direction in the Upper Yangtze region
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图 7 上扬子地区平行裂陷方向下寒武统地层厚度分布
Fig. 7 Isopach maps of the Lower Cambrian (a) Maidiping and (b) Qiongzhusi formations parallel to the rift direction in the Upper Yangtze region
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图 8 上扬子地区平行裂陷方向下寒武统筇竹寺组不同亚段地层厚度分布
(a) 筇一1亚段；(b) 筇一2亚段；(c) 筇一3亚段；(d) 筇一4亚段；(e) 筇二1+筇二2亚段；(f) 筇二3+筇二4亚段
Fig. 8 Isopach maps of various sub-members of the Lower Cambrian Qiongzhusi Formation parallel to the rift direction in the Upper Yangtze region
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图 10 扫描电镜照片展示上扬子地区下寒武统筇竹寺组黑色页岩孔隙特征
(a) 资201井，4 754.23 m；(b) 资201井，4 781.23 m；(c) 威207井，3 022.07 m；(d) 资201井，4 556.99 m
Fig. 10 Scanning electron microscope (SEM) images showing the pore characteristics of black shales in the Lower Cambrian Qiongzhusi Formation, Upper Yangtze region
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图 11 上扬子地区下寒武统筇竹寺组筇二1孔隙率变化关系
Fig. 11 Porosity variations in the Q2-1 sub-member of the Lower Cambrian Qiongzhusi Formation, Upper Yangtze region
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图 12 上扬子地区下寒武统麦地坪和筇竹寺组地层分布模式及页岩气成藏特征
Fig. 12 Stratigraphic distribution pattern and shale gas accumulation characteristics of the Lower Cambrian Maidiping and Qiongzhusi formations, Upper Yangtze region
表 1 上扬子地区下寒武统相关的地层划分方案[5]
Table 1 Stratigraphic subdivision scheme for the Lower Cambrian in the Upper Yangtze region[5]
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表 2 上扬子地区下寒武统麦地坪组—筇竹寺组地层划分及特征
Table 2 Stratigraphic subdivision and characteristics of the Lower Cambrian Maidiping and Qiongzhusi formations, Upper Yangtze region
地层 岩性特征 电性特征 沉积相 生物组合 沧浪铺组 深灰色薄层页岩及粉砂质泥岩、泥质粉砂岩互层 自然伽马和声波均呈低值锯
齿状，电阻率振荡增大潮坪相 筇竹寺组 筇二段 筇二4 浅灰色粉砂质泥岩、
泥质粉砂岩互层箱状低自然伽马和声波，
电阻率较大、平直状浅水陆棚 Parabadiella-MianxiandiscusEoredlichia-Wutingaspis 筇二3 灰色泥岩、粉砂质泥岩 漏斗状低自然伽马和声波，
电阻率较大、平直状浅水陆棚 筇二2 浅灰色页岩，
夹有少量粉砂岩漏斗状中自然伽马，中声波，平直状中高电阻率 深水陆棚 Lapworthella-Tannuolina-Sinoscachites 筇二1 黑色、深灰色页岩、
炭质页岩，夹有少量粉砂岩指状中高自然伽马，高声波，平直状中高电阻率 深水陆棚 筇一段 筇一4 深灰色泥质砂岩、粉砂岩，夹少量灰岩及泥岩 箱形低自然伽马和声波，
电阻率较大、平直状浅水陆棚 筇一3 黑色炭质页岩 中高自然伽马、高声波，
中低电阻率深水陆棚 筇一2 灰黑色粉砂质页岩与
泥岩互层箱形低自然伽马和声波，
齿状低电阻浅水陆棚 筇一1 黑色炭质页岩、粉砂质页岩 中高自然伽马和声波，
中高指状电阻率深水陆棚 麦地坪组 硅质页岩、白云岩、
磷块岩等自然伽马值高低相间、
中高电阻深水坳拉槽 Anabarites trisulcatus-Protohertzina anabarica带、Siphogonuchites pusilliformis-Paragloborilus subglobosus带、Heraultipegma yunnanensis带 灯影组 白云岩 低伽马、高电阻 碳酸盐岩台地相
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表 3 上扬子地区下寒武统麦地坪组—筇竹寺组不同层段页岩矿物组成
Table 3 Mineral compositions of shales in different intervals of the Lower Cambrian Maidiping and Qiongzhusi formations, Upper Yangtze region
% 层位 黏土总量 石英 正长石 斜长石 方解石 白云石 黄铁矿 菱铁矿 沧浪铺组 37.2 39.3 0 7.8 15.8 1.5 1.5 0 筇二4 35.4 38.1 0.9 9.1 14.0 2.4 2.5 0 筇二3 35.8 31.8 1.4 11.4 8.7 7.2 3.7 0 筇二2 21.3 45.6 2.4 21.1 3.5 4.3 1.8 0 筇二1 23.6 38.4 3.7 23.3 3.1 3.8 4.2 0 筇一4 15.6 39.6 4.5 25.5 9.8 3.4 1.8 0 筇一3 25.9 34.3 4.7 12.3 3.7 9.7 9.4 0 筇一2 33.0 33.5 3.5 18.0 9.5 0.0 2.5 0 筇一1 5.5 68.1 0.9 3.2 6.4 2.3 6.6 7 麦地坪组 11.4 56.2 0 5.7 1.2 5.4 11.1 9.15
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