Shale sedimentary environments and their controlling factors in Lianggaoshan Formation of Fuxing area, Sichuan Basin
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摘要: 以四川盆地复兴地区侏罗系凉高山组二段(凉二段)页岩为研究对象，综合运用地球化学与沉积学分析，系统揭示了研究区页岩沉积期古环境特征及其对页岩品质的控制作用，并建立了页岩沉积模式。凉高山组页岩沉积期，水体呈淡水—半咸水环境，古水深介于4.9~39.4 m(平均值17.2 m)，古生产力水平较高(生物钡平均含量为567.24 ug/g)，整体呈厌氧还原环境，总体上为温暖潮湿气候。研究区凉高山组页岩总有机碳(TOC)含量受控于古水深、古盐度、古生产力和古氧化还原环境，水体越深、盐度越高、生产力越高、气候越温暖潮湿，TOC含量越高。在还原条件背景下，微弱的氧化还原环境差异对TOC含量影响不大。凉二段下亚段沉积期上气层较下气层水体更深、古生产力更高、古气候更偏温暖潮湿，有机质更富集。在此基础上，建立了研究区凉二段下亚段页岩沉积模式：下气层沉积期，在淡水—半咸水、半潮湿—半干旱气候、中等古生产力、厌氧还原条件下，主要沉积一般—中等品质页岩；上气层沉积期，在淡水—半咸水、温暖潮湿气候，中等—高古生产力、厌氧还原条件下，主要沉积中等—优质页岩。Abstract: Taking the shale in the second member of the Jurassic Lianggaoshan Formation (Liang 2) in the Fuxing area of the Sichuan Basin as the research object, this study employed geochemical and sedimentary analysis to systematically investigate the paleoenvironmental characteristics of the shale in the study area during the sedimentary period and their controlling effects on shale quality. Sedimentary models for the shale were established. The results showed that the shale in the Lianggaoshan Formation was deposited in a freshwater to brackish water environment with a paleo-water depth of 4.9 to 39.4 m, averaging 17.2 m. The paleo-productivity level was high with an average bio-barium content of 567.24 μg/g. The overall environment was anaerobic and reducing, and the climate was warm and humid in general. The total organic carbon (TOC) content of the shale in the Lianggaoshan Formation was controlled by paleo-water depth, paleosalinity, paleoproductivity, and paleo-water redox environment. Higher TOC content was positively correlated with water depth, salinity, productivity, and warm and humid climate. Under redox conditions, minor differences in reducing environments had little impact on TOC content. During the sedimentary period of the lower sub-member of Liang 2, the upper gas layers had a deeper water body, higher paleoproductivity, and a warmer, more humid paleoclimate compared to the lower gas layers, resulting in richer organic matter accumulation. Based on these findings, two types of shale sedimentary models were established for shale in the lower sub-member of the Liang 2 in the study area: (1) As the lower gas layers deposited, under freshwater to brackish water, semi-humid to semi-arid climate, moderate paleoproductivity, and anaerobic-reducing conditions, fair to medium-quality shale was mainly deposited. (2) As the upper gas layers deposited, under freshwater to brackish water, warm and humid climate, moderate to high paleoproductivity, and anaerobic-reducing conditions, medium to high-quality shale was primarily deposited.
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Key words:
- shale quality /
- sedimentary environment /
- controlling factor /
- Lianggaoshan Formation /
- Fuxing area /
- Sichuan Basin
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图 1 四川盆地构造分区及研究区位置
Figure 1. Tectonic division of Sichuan Basin and location of study area
图 2 四川盆地复兴地区A井凉高山组综合柱状图
Figure 2. Comprehensive histogram of Lianggaoshan Formation of well A in Fuxing area, Sichuan Basin
图 3 四川盆地复兴地区凉高山组页岩矿物(a)和黏土矿物(b)含量分布
Figure 3. Shale mineral (a) and clay mineral (b) composition of Lianggaoshan Formation in Fuxing area, Sichuan Basin
图 4 四川盆地复兴地区凉高山组页岩岩相划分图
Figure 4. Shale lithofacies division of Lianggaoshan Formation in Fuxing area, Sichuan Basin
图 5 四川盆地复兴地区凉高山组页岩典型岩相类型
Figure 5. Typical shale lithofacies types of Lianggaoshan Formation in Fuxing area, Sichuan Basin
图 6 四川盆地复兴地区A井凉高山组页岩地球化学特征垂向变化
Figure 6. Vertical variation trend of geochemical characteristics of shale in Lianggaoshan Formation in well A of Fuxing area, Sichuan Basin
图 7 四川盆地复兴地区凉高山组页岩干酪根碳同位素与埋深交会图
Figure 7. Kerogen carbon isotopes vs. burial depth of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 8 四川盆地复兴地区凉高山组页岩古盐度指标垂向变化
Figure 8. Vertical variation trend of palaeosalinity indicators of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 9 四川盆地复兴地区凉高山组页岩典型岩心、沉积构造及古生物标志
Figure 9. Typical cores, sedimentary structures, and paleontological markers of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 10 四川盆地复兴地区凉高山组页岩古水深指标垂向变化
Figure 10. Vertical variation trend of paleo-water depth of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 11 四川盆地复兴地区凉高山组页岩古气候指标垂向变化
Figure 11. Vertical variation trend of paleoclimate of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 12 四川盆地复兴地区凉高山组页岩古生产力指标垂向变化
Figure 12. Vertical variation trend of palaeoproductivity of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 13 四川盆地复兴地区凉高山组页岩氧化还原性指标垂向变化
Figure 13. Vertical variation trend of redox indicators of shale in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 14 四川盆地复兴地区凉高山组页岩TOC与沉积环境指标相关性分析
Figure 14. Sedimentary environment indicators vs. shale TOC content in Lianggaoshan Formation of Fuxing area, Sichuan Basin
图 15 四川盆地复兴地区凉高山组页岩沉积模式
Figure 15. Shale sedimentary models of Lianggaoshan Formation in Fuxing area, Sichuan Basin
表 1 四川盆地复兴地区凉高山组页岩样品测试项目统计表
Table 1. Test items of shale samples from Lianggaoshan Formation in Fuxing area, Sichuan Basin
井号 采样深度/m ω(TOC)/% 测试项目次数/次 岩石热解 干酪根碳同位素 薄片鉴定 全岩X衍射 黏土X衍射 Ro 金属元素 稀土元素 A 2 527~2 608 81 81 20 40 81 40 8 56 56 B 2 681~2 745 64 64 14 30 64 30 6 87 87 C 2 576~2 641 65 65 15 32 65 32 6 73 73 D 2 406~2 465 59 59 12 30 59 30 6 64 64 
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表 2 四川盆地复兴地区凉高山组页岩有机质丰度统计表
Table 2. Shale organic matter abundance in Lianggaoshan Formation of Fuxing area, Sichuan Basin
层位 ω(TOC)/% S1+S2/(mg/g) 页岩品质 凉二段下亚段上气层 0.44~3.09/1.51 0.77~5.37/1.86 中等—优质 凉二段下亚段下气层 0.24~2.56/1.21 0.36~4.28/1.24 差—中等 注：表中数值的意义为：最小值~最大值/平均值。
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