Micropore Characteristics and Genesis of Shale Reservoirs in Coal Measures in Huainan Coalfield
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摘要: 煤系泥页岩储层发育的微孔（孔径<2 nm）对泥页岩气吸附赋存具有重要意义。以淮南煤田石炭—二叠纪海相-海陆过渡相煤系泥页岩为研究对象，通过Ro，max、TOC、XRD和CO2吸附实验，揭示储层微孔结构特征，探讨微孔发育的控制因素及成因。研究表明：太原组、山西组和下石盒子组泥页岩有机质成熟度基本接近，处于低成熟-成熟阶段；三角洲平原亚相的下石盒子组TOC最高、黏土矿物最丰富、微孔最发育，其次为障壁砂坝-澙湖相的太原组，三角洲前缘和前三角洲亚相的山西组TOC最低，黏土矿物中等，微孔最不发育；微孔孔径分布发育峰1（0.366 5 nm）、峰2（0.457 7~0.627 2 nm）和峰3（0.821 6 nm）三个峰或区间。微孔孔容与TOC以及黏土矿物（高岭石和绿泥石）含量呈正相关，与脆性矿物含量呈负相关，推断储层主要发育有机质孔和黏土矿物孔，不同类型微孔的发育受控于不同沉积环境及成岩演化下有机碳含量和矿物成分差异。峰1对应微孔归因于黏土矿物孔为主，有机质孔少量，峰2为黏土矿物孔和有机质孔共同主导，峰3主要为有机质孔，少量黏土矿物孔；认为有机质孔为芳环层间孔（峰1+峰2）和芳环有序堆叠形成的柱状孔（峰3），黏土矿物孔为高岭石和绿泥石矿物内部片层之间的空穴或经后期转化改造形成的微孔，以上也可能在有机质与黏土矿物的复合体中发育微孔。Abstract: The micropores (pore width < 2 nm) developed in shale reservoirs in coal measures are of great significance to the adsorption and occurrence of mud shale gas. This paper studied the marine-continental Carboniferous-Permian mud shale reservoirs in coal measures in Huainan Coalfield by the experiments of Ro,max, TOC, XRD and CO2 adsorption. The micropore structure characteristics of reservoirs were revealed and the controlling factors and genesis were discussed. The results show that the maturity of organic matters in Taiyuan Formation, Shanxi Formation and Lower Shihezi Formation is between low mature and mature stage. Lower Shihezi Formation, deposited in the delta-plain, has the highest content of TOC and clay mineral, and the micropores are the most developed one in the three formations, followed by barrier dams-lagoon facies of Taiyuan Formation. Shanxi Formation, deposited in the delta front and pro-delta facies, has the lowest content of TOC, moderate content of clay mineral, and the least developed micropores. There are three peaks in micropore width distribution, namely peak 1 (0.366 5 nm), peak 2 (0.457 7-0.627 2 nm) and peak 3 (0.821 6 nm). Micropore volume has a positive correlation with the content of TOC and clay minerals, but a negative correlation with the content of brittle minerals. Therefore, it is concluded that the reservoirs mainly develop micropores of organic matters and clay minerals. The development of different types of micropores is controlled by different content of organic carbon and mineral composition under different types of sedimentary environment and diagenetic evolution. Micropores of peak 1 are attributed to the main pores of clay minerals and a small number of organic matter pores; peak 2 are dominated by both clay mineral pores and organic matter pores; peak 3 are mainly organic matter pores and a small amount of clay mineral pores. Organic matter micropores of peak 1 + peak 2 are supposed to be corresponding to aromatic ring interlayers pores, and peak 3 are columnar pore formed by the ordered stacking of aromatic ring or others. The micropores in clay minerals are in the internal layer of kaolinite and chlorite or the micropores formed in the late diagenesis transformation. All the above micropores may also developed in the complex of organic matters and clay minerals.
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