Coupling between Source Rock and Reservoir of Shale Gas in Wufeng-Longmaxi Formation in Sichuan Basin, South China

: In order to analyze the main factors controlling shale gas accumulation and to predict the potential zone for shale gas exploration, the heterogeneous characteristics of the source rock and reservoir of the Wufeng-Longmaxi Formation in Sichuan Basin were discussed in detail, based on the data of petrology, sedimentology, reservoir physical properties and gas content. On this basis, the effect of coupling between source rock and reservoir on shale gas generation and reservation has been analyzed. The Wufeng-Longmaxi Formation black shale in the Sichuan Basin has been divided into 5 types of lithofacies, i.e., carbonaceous siliceous shale, carbonaceous argillaceous shale, composite shale, silty shale, and argillaceous shale, and 4 types of sedimentary microfacies, i.e., carbonaceous siliceous deep shelf, carbonaceous argillaceous deep shelf, silty argillaceous shallow shelf, and argillaceous shallow shelf. The total organic carbon (TOC) content ranged from 0.5% to 6.0% (mean 2.54%), which gradually decreased vertically from the bottom to the top and was controlled by the oxygen content of the bottom water. Most of the organic matter was sapropel in a high-over thermal maturity. The shale reservoir of Wufeng-Longmaxi Formation was characterized by low porosity and low permeability. Pore types were mainly <10 nm organic pores, especially in the lower member of the Longmaxi Formation. The size of organic pores increased sharply in the upper member of the Longmaxi Formation. The volumes of methane adsorption were between 1.431 m 3 /t and 3.719 m 3 /t, and the total gas contents were between 0.44 m 3 /t and 5.19 m 3 /t, both of which gradually decreased from the bottom upwards. Shale with a high TOC content in the carbonaceous siliceous/argillaceous deep shelf is considered to have signiﬁcant potential for hydrocarbon generation and storage capacity for gas preservation, providing favorable conditions of the source rock and reservoir for shale gas.


Introduction
During the Late Ordovician to Early Silurian, massive black shale ("hot shale") was deposited worldwide under the shelf and epicontinental environment with sea levels rising due to melting icebergs [1][2][3]. The Wufeng-Longmaxi Formation black shale (WLBS) in the Sichuan Basin are the equivalent strata of hot shale in south China, which are the main target strata for shale gas exploration and development in China [4,5]. The proved shale gas reserves in the WLBS exceed 5000 × 10 8 m 3 [6]. The strata in the upper Ordovician-lower Silurian is one of the most widely developed high-quality source rocks in the world. The shale of the Wufeng-Longmaxi Formation deposited during this period in South China has a high content of organic matter and stable lateral distribution [7][8][9]. Shale gas reservoirs are characterized by low porosity and low permeability, with small pore size and abundant nanopores (about 10 nm in diameter) [10].
At present, significant breakthroughs have been achieved in shale gas exploration in the Sichuan Basin (e.g., in Fuling, Weiyuan-Changning), and the largest shale gas field in China has been built in Fuling. Previous studies have proved that the enrichment of marine shale gas in South China is mainly controlled by 3 factors: (1) shale in the deep shelf provided the material basis for shale gas generation [7,[11][12][13]; (2) the moderate thermal evolution was conducive to the formation of organic pores, which provided available storage spaces for shale gas [14][15][16]; (3) the favorable preservation condition is the key condition for the enrichment of shale gas [17,18]. As an unconventional resource, shale gas was generated and accumulated in organic-rich shale; thus, organic-rich shale is considered as both the resource rock and reservoir [19][20][21].
However, previous research on shale was mainly focused on the source rock or reservoirs separately, e.g., the quantity of hydrocarbon generation or quality of reservoirs. In recent work, overwhelming evidence proves that high organic content and high porosity appear simultaneously in shale [15,[22][23][24], which is different from a conventional oil-gas reservoir. The geological characteristics of shale could determine the material basis for shale gas generation, as well as provide storage space for shale gas preservation [25,26]. Therefore, the favorable combination of hydrocarbon source rock and reservoir is an important condition for shale gas accumulation. However, the study on the coupling characteristics of shale gas source rocks and reservoirs is still insufficient and needs more detailed work.
In this study, the heterogeneous characteristics of organic and inorganic components in the source rock and reservoir of the WLBS in the Sichuan Basin are discussed in detail, based on petrology, sedimentology, reservoir physical properties, and gas content. On this basis, the effect of coupling between the source rock and reservoir on shale gas generation and reservation was analyzed. It would be helpful to analyze the main factors controlling shale gas accumulation and to predict the potential zone for shale gas exploration.

Materials and Methods
A total of 173 samples were collected from cores of well A for various experiments and 26 samples from other wells in the Sichuan Basin ( Figure 1) for capturing scanning electron microscope (SEM) images and focused ion beam (FIB) SEM images. Rock thin sections were performed at the Geological Exploration and Development Research Institute, Experimental Research Center, Chuanqing Drilling Engineering Co., LTD, CNPC, Chuanqing, China. The SEM images were made at the State Key Laboratory of Biochemical Engineering, Institute of Process Engineering, Chinese Academy of Sciences, and at the State Key Laboratory of Shale Oil and Gas Enrichment Mechanisms and Effective Development, SINOPEC. Three-dimensional FIB SEM images were made at China University of Petroleum (Beijing, China). Physical properties in the reservoir were determined at the State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation, Chengdu University of Technology. Physical properties in the reservoir were determined at the State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation, Chengdu University of Technology. The threedimensional FIB SEM images were made with a FEI-Helios NanoLab 650 under the testing condition of 30.0 KV and 9.3 nA (I-beam), 5.0 KV and 0.4 nA (E-beam). The experiment of mineral composition was conducted at National Geological Testing Center. The data of mineral composition were measured with D8 ADVANCE XRD Diffractometer by the individual spectra of the anticipated mineral components. Organic geochemical analyses were performed at SINOPEC. The kerogen was extracted from shale samples through acid dissolving (HCl and HF) and drying, which was used to test organic carbon isotopes and organic types. The experiment of kerogen carbon isotope with GC-C-IRMS (DELTA

Mineral Composition
Based on the data of mineral composition, quartz was determined to be the dominated mineral composition in the WLBS (from 30-70%, with an average of 42%), followed by clay minerals (from 20-50%, with an average of 36%), with a small amount of carbonate minerals ( Figure 2).

Mineral Composition
Based on the data of mineral composition, quartz was determined to be the dominated mineral composition in the WLBS (from 30-70%, with an average of 42%), followed by clay minerals (from 20-50%, with an average of 36%), with a small amount of carbonate minerals ( Figure 2).

Mineral Composition
Based on the data of mineral composition, quartz was determined to be the dominated mineral composition in the WLBS (from 30-70%, with an average of 42%), followed by clay minerals (from 20-50%, with an average of 36%), with a small amount of carbonate minerals ( Figure 2).

Organic Geochemistry
The values of vitrinite reflectance (Ro) from nine samples in Well A ranged from 2.2% to 3.13%, and the values of δ 13 C org are −29.2 % and −29.3 % , respectively ( Figure 3, Table 1). The values of total organic carbon (TOC) in WLBS of Well A basically ranged from 0.5% to 6.0% (about 2.54% on average) and gradually decreased vertically from the bottom to the top ( Figure 3).  Figure 3, Table 1). The values of total organic carbon (TOC) in WLBS of Well A basically ranged from 0.5% to 6.0% (about 2.54% on average) and gradually decreased vertically from the bottom to the top ( Figure 3).

Reservoir Properties
The porosity of the WLBS in Well A ranged from 1.17% to 8.61% (mean 4.78%), and the permeability was basically distributed between 0.0015 mD and 335.21 mD (Figure 3). On the whole, the reservoir of WLBS is characterized by low porosity and low permeability.

Methane Adsorption
With the increase of pressure in the experiment, the absorbed gas of methane in the shale reservoir increased gradually. The quantities of methane adsorption from Well A ranged between 1.42 m 3 /t and 3.66 m 3 /t under the maximum pressure of 10.83 MPa ( Table 2). The maximum adsorption of methane under equilibrium (Langmuir volume) was between 1.72 m 3 /t and 4.66 m 3 /t (Table 2), calculated by the Langmuir equation.

Types of Lithofacies
An obvious positive relationship existed between quartz and TOC, in which the Pearson correlation coefficient was 0.7099 ( Figure 4). In the vertical direction, the content of quartz gradually decreased from bottom to top, while the content of clay minerals gradually increased ( Figure 3). Previous research believed that the quartz in the lower member of WLBS was mainly of biogenetic origin [4,28], which could be proved by the picture of quartz with biogenic structure under the microscope (Figure 5a,b).
Lithofacies is a kind of rock or rock assemblage formed in a certain sedimentary environment. On the basis of the characteristics of the rock mineral composition, the TOC content, core descriptions (e.g., structure), and microscopic identification of rock thin sections (e.g., abundance of fossils), the WLBS in the study area was divided into 5 types of lithofacies as follows (Table 3).

Carbonaceous siliceous shale (LF1):
The color was normally dark grey-black in this lithofacies. The quartz content was close to or >50% and was mainly of a biogenetic origin, whereas the content of clay minerals and carbonate minerals was very low (Figures 3  and 5a,b). The organic matter content was high (TOC 3-4%) with massive fossils of graptolites. Horizontal laminations occurred frequently in LF1, which was mainly deposited during the transgression stage and was found to be distributed in the Wufeng Formation and lower member of the Longmaxi Formation ( Figure 3).
Carbonaceous argillaceous shale (LF2): The color of this lithofacies was dark greyblack. The quartz content was normally between 30% and 50%, whereas the TOC content ranged from 2% to 3% (Figures 3 and 5c,d). LF2 was mainly deposited during the transgression stage and was found to be distributed in the lower member of the Longmaxi Formation ( Figure 3).
Composite shale (LF3): The color of this shale was dark grey. The contents of silicate, clay minerals and carbonate minerals in this lithology were relatively similar (Figures 3 and 5e-h). The organic matter content (TOC 1.0-2.5%) was lower in comparison to LF1 and LF2. LF3 was mainly deposited during the stage of the early high-stand system tract and was observed to be distributed in the middle and upper members of the Longmaxi Formation ( Figure 3).
Silty shale (LF4): The color of this lithofacies was dark grey. The quartz was derived from terrestrial silty particles and the content of clay minerals was <50% (Figures 3 and 5i,j). Graptolites fossils were scarce and the TOC content ranged from 1.0% to 2.0%. Silty bands or horizontal layers can be found in LF4. This was mainly deposited during the stage of the late high-stand system tract and was found to be distributed in the middle and upper member of the Longmaxi Formation ( Figure 3). Argillaceous shale (LF5): The color of this shale was dark grey. The content of clay minerals was between 40% and 50%, whereas the contents of carbonate minerals were relatively low (Figures 3 and 5k,l). The TOC content was about 1% and only a few fossils (e.g., graptolites) were found. LF5 was mainly deposited during the stage of the late high-stand system tract and was observed to be distributed in the upper member of the Longmaxi Formation ( Figure 3).

Types of Sedimentary Microfacies
In combination with information regarding the regional geological background, lithofacies, and symbols of sedimentary facies, the WLBS was divided into 4 types of sedimentary microfacies as follows (Table 4).   Carbonaceous siliceous shale (LF1): The color was normally dark grey-black in this lithofacies. The quartz content was close to or >50% and was mainly of a biogenetic origin, whereas the content of clay minerals and carbonate minerals was very low (Figures 3 and 5a,b). The organic matter content was high (TOC 3-4%) with massive fossils of graptolites. Horizontal laminations occurred frequently in LF1, which was mainly deposited during the transgression stage and was found to be distributed in the Wufeng Formation and lower member of the Longmaxi Formation ( Figure 3).
Carbonaceous argillaceous shale (LF2): The color of this lithofacies was dark greyblack. The quartz content was normally between 30% and 50%, whereas the TOC content ranged from 2% to 3% (Figures 3 and 5c,d). LF2 was mainly deposited during the transgression stage and was found to be distributed in the lower member of the Longmaxi Formation ( Figure 3).
Composite shale (LF3): The color of this shale was dark grey. The contents of silicate, clay minerals and carbonate minerals in this lithology were relatively similar (Figures 3 and 5e-h). The organic matter content (TOC 1.0-2.5%) was lower in comparison to LF1 and LF2. LF3 was mainly deposited during the stage of the early high-stand system tract and was observed to be distributed in the middle and upper members of the Longmaxi Formation ( Figure 3).
Silty shale (LF4): The color of this lithofacies was dark grey. The quartz was derived from terrestrial silty particles and the content of clay minerals was <50% (Figures 3 and 5i,j). Graptolites fossils were scarce and the TOC content ranged from 1.0% to 2.0%. Silty bands or horizontal layers can be found in LF4. This was mainly deposited during the stage of the late high-stand system tract and was found to be distributed in the middle and upper member of the Longmaxi Formation ( Figure 3).
Argillaceous shale (LF5): The color of this shale was dark grey. The content of clay minerals was between 40% and 50%, whereas the contents of carbonate minerals were relatively low (Figures 3 and 5k,l). The TOC content was about 1% and only a few fossils (e.g., graptolites) were found. LF5 was mainly deposited during the stage of the late high-stand system tract and was observed to be distributed in the upper member of the Longmaxi Formation ( Figure 3).

Types of Sedimentary Microfacies
In combination with information regarding the regional geological background, lithofacies, and symbols of sedimentary facies, the WLBS was divided into 4 types of sedimentary microfacies as follows (Table 4).  level, which was evident from the occurrence of frequent pyrite bands and aggregations.
Carbonaceous argillaceous deep shelf (SMF2): This microfacies mainly consisted of LF2 and LF3, and was mainly developed in the lower member of Longmaxi Formation (Figure 3). The sedimentary environment was mainly anoxic as there was a decreased sea-level in comparison to SMF1.
Silty argillaceous shallow shelf (SMF 3): This microfacies mainly consisted of LF4 interbedded with some of LF5, and was developed in the middle and upper members of the Longmaxi Formation (Figure 3). The sedimentary environment was mainly oxidizing due to a low sea-level.
Argillaceous shallow shelf (SMF4): This microfacies mainly consisted of LF5 interbedded with some of LF4, and was mainly developed in the middle and upper member of the Longmaxi Formation (Figure 3). The sedimentary environment was mainly oxicanoxic with low sea level.

Characteristics of Organic Geochemistry
Remarkable differences in organic matter content were observed among the different sedimentary microfacies (Figure 6), whereby the TOC values in SMF1 were normally >4%, whereas those in SMF2 were between 2% and 4%, and those in SMF3 and SMF4 were mostly <2%. Generally, the shale in SMF1 (followed by SMF2) was beneficial for the accumulation of organic matter, whereas the shale in SMF3 and SMF4 was not.
due to a low sea-level.
Argillaceous shallow shelf (SMF4): This microfacies mainly consisted of terbedded with some of LF4, and was mainly developed in the middle and upp ber of the Longmaxi Formation (Figure 3). The sedimentary environment was oxic-anoxic with low sea level.

Characteristics of Organic Geochemistry
Remarkable differences in organic matter content were observed among the sedimentary microfacies (Figure 6), whereby the TOC values in SMF1 were norma whereas those in SMF2 were between 2% and 4%, and those in SMF3 and SM mostly <2%. Generally, the shale in SMF1 (followed by SMF2) was beneficial fo cumulation of organic matter, whereas the shale in SMF3 and SMF4 was not.
The accumulation of organic matter in marine shale is the result of various f the sedimentary environment. It is generally believed that the main controlling f organic matter accumulation are preservation condition (anoxic bottom water) a primary productivity [29,30]. Previous studies suggested that large-scale trans occurred during the Early Silurian due to the melting of glaciers, which caused ocean anoxic event [31,32]. The SMF1 at the bottom of the Longmaxi Formation e the transgression systems tract with a strongly reducing environment, thus resul large amount of organic matter preservation. Subsequently, the oxygen conten bottom water gradually increased due to decreasing sea level; therefore, the matter in SMF2, SMF3, and SMF4 decreased accordingly. Previous studies suggested that the WLBS experienced a long burial period, multiple periods of tectonic evolution occurred in the Sichuan Basin, which have in the deep burial depth of the WLBS. Other studies reported that Ro values ran tween 2.4% and 4.0%, indicating the organic matter was over-mature [33,34] study, Ro values from eight samples in Well A ranged from 2.2% to 3.13% and that the organic matter was also in the stage of high -over maturity in study area The accumulation of organic matter in marine shale is the result of various factors in the sedimentary environment. It is generally believed that the main controlling factors of organic matter accumulation are preservation condition (anoxic bottom water) and high primary productivity [29,30]. Previous studies suggested that large-scale transgression occurred during the Early Silurian due to the melting of glaciers, which caused a severe ocean anoxic event [31,32]. The SMF1 at the bottom of the Longmaxi Formation existed in the transgression systems tract with a strongly reducing environment, thus resulting in a large amount of organic matter preservation. Subsequently, the oxygen content in the bottom water gradually increased due to decreasing sea level; therefore, the organic matter in SMF2, SMF3, and SMF4 decreased accordingly.
Previous studies suggested that the WLBS experienced a long burial period, and that multiple periods of tectonic evolution occurred in the Sichuan Basin, which have resulted in the deep burial depth of the WLBS. Other studies reported that Ro values ranged between 2.4% and 4.0%, indicating the organic matter was over-mature [33,34]. In this study, Ro values from eight samples in Well A ranged from 2.2% to 3.13% and indicate that the organic matter was also in the stage of high -over maturity in study area, as well ( Figure 3, Table 1). Both δ 13 C values for kerogen from Well A were >−29% (Table 1), thus implying that the kerogens in the WLBS are sapropel (type I), as based on comparing them with the classification standard of kerogen type (Huang et al., 1984). Moreover, the microscope images of extracted kerogens also evidenced that the organic matter was flocculent sapropel derived from algae (Figure 7).
Energies 2021, 14, x FOR PEER REVIEW 9 of 1 ( Figure 3, Table 1). Both δ 13 C values for kerogen from Well A were >−29‰ (Table 1), thu implying that the kerogens in the WLBS are sapropel (type Ⅰ), as based on comparin them with the classification standard of kerogen type (Huang et al., 1984). Moreover, th microscope images of extracted kerogens also evidenced that the organic matter wa flocculent sapropel derived from algae ( Figure 7).

Types of Pores in Reservoir
In this study, massive SEM images of the WLBS were observed to classify the type of pores on the basis of pore origins. By analyzing the origins of the pores, the pore could be divided into 5 types.
Organic pore: Shapes were observed to be largely irregular, spherical, or slit, an diameters were mainly in nanoscale. The organic pores formed during the hydrocarbo generation in organic matter attached among the inorganic particles (Figure 8a,b). Thi type of pore is abundant in LF1-2 and SMF1-2, where organic matter was rich and hy drocarbons were readily generated.
Interbedded pore of clay minerals: Shapes were observed to be mostly plate-like layered, reticulate, linear, or irregular, and diameters ranged from hundreds of na nometers to the millimeter level. These pores were mainly generated between layers o clay minerals such as illite or chlorite during the process of diagenetic transformation o alteration (Figure 8c,d). This type of pore is abundant in LF5 and SMF4, in which th contents of clay minerals were relative high.
Intergranular pore: Shapes were observed to be largely triangular, polygonal, o irregular, and diameters were in nanoscale. Intergranular pores were mainly residua primary pores after diagenetic compaction, and were mostly found among particles o quartz, feldspar, and clay minerals (Figure 8e,f). This type of pore could be found in a the lithofacies and microfacies.
Intragranular pore: Shapes were observed to be mostly elliptic, linear, or irregula and diameters were in nanoscale. Intragranular pores were mainly formed by diagenesi (e.g., transformation, alteration, and dissolution) in particles of quartz, feldspar, calcite apatite, and other minerals (Figure 8g-i). This type of pore could be found in all th lithofacies and microfacies.
Microfractures: Shapes were observed to be largely linear and serrated, and length ranged from hundreds of nanometers to the millimeter level. These microfractures wer formed by 3 origins: (1) tensile microfractures generated under tectonic activities; (2 microfractures around rigid particles that were formed by the shrinkage of mineral par ticles during diagenesis; and (3) microfractures in organic matter that were formed due t the overpressure during hydrocarbon generation (Figure 8j-l). The tensile microfracture and microfractures around rigid particles appear occasionally, and the microfractures i organic matter occur frequently in LF1-2 and SMF1-2.

Types of Pores in Reservoir
In this study, massive SEM images of the WLBS were observed to classify the types of pores on the basis of pore origins. By analyzing the origins of the pores, the pores could be divided into 5 types.
Organic pore: Shapes were observed to be largely irregular, spherical, or slit, and diameters were mainly in nanoscale. The organic pores formed during the hydrocarbon generation in organic matter attached among the inorganic particles (Figure 8a,b). This type of pore is abundant in LF1-2 and SMF1-2, where organic matter was rich and hydrocarbons were readily generated.
Interbedded pore of clay minerals: Shapes were observed to be mostly plate-like, layered, reticulate, linear, or irregular, and diameters ranged from hundreds of nanometers to the millimeter level. These pores were mainly generated between layers of clay minerals such as illite or chlorite during the process of diagenetic transformation or alteration (Figure 8c,d). This type of pore is abundant in LF5 and SMF4, in which the contents of clay minerals were relative high.
Intergranular pore: Shapes were observed to be largely triangular, polygonal, or irregular, and diameters were in nanoscale. Intergranular pores were mainly residual primary pores after diagenetic compaction, and were mostly found among particles of quartz, feldspar, and clay minerals (Figure 8e,f). This type of pore could be found in all the lithofacies and microfacies.
Intragranular pore: Shapes were observed to be mostly elliptic, linear, or irregular, and diameters were in nanoscale. Intragranular pores were mainly formed by diagenesis (e.g., transformation, alteration, and dissolution) in particles of quartz, feldspar, calcite, apatite, and other minerals (Figure 8g-i). This type of pore could be found in all the lithofacies and microfacies.
Microfractures: Shapes were observed to be largely linear and serrated, and lengths ranged from hundreds of nanometers to the millimeter level. These microfractures were formed by 3 origins: (1) tensile microfractures generated under tectonic activities; (2) microfractures around rigid particles that were formed by the shrinkage of mineral particles during diagenesis; and (3) microfractures in organic matter that were formed due to the overpressure during hydrocarbon generation (Figure 8j-l). The tensile microfractures and microfractures around rigid particles appear occasionally, and the microfractures in organic matter occur frequently in LF1-2 and SMF1-2.

Porosity and Permeability
The porosity of the lower member of the WLBS was mostly between 4% and 6%, whereas that of the middle member of the WLBS was generally <4% and that of the upper member of the WLBS was between 4% and 8% ( Figure 3). The variation of permeability was relatively larger (0.0015-335.21 mD) due to microfractures in some samples (Figure 3), which provided infiltration channels conducive to shale gas production.
Overall, porosity showed a positive relationship with TOC, in which the Pearson correlation coefficient is 0.5725 (Figure 9a), which indicated the increase of organic pores make the porosity increase simultaneously. The upper member of the WLBS had a high porosity, low TOC, and high content of clay minerals, thus implying that the interbedded pores of clay minerals contribute to massive pores. Furthermore, porosity was positively correlated with Ro values, in which the Pearson correlation coefficient is 0.7589 (Figure 9b), which indicated that pores in the shale reservoir gradually increased with the advancement of thermal evolution.

Porosity and Permeability
The porosity of the lower member of the WLBS was mostly between 4% and 6%, whereas that of the middle member of the WLBS was generally <4% and that of the upper member of the WLBS was between 4% and 8% ( Figure 3). The variation of permeability was relatively larger (0.0015-335.21 mD) due to microfractures in some samples (Figure 3), which provided infiltration channels conducive to shale gas production.
Overall, porosity showed a positive relationship with TOC, in which the Pearson correlation coefficient is 0.5725 (Figure 9a), which indicated the increase of organic pores make the porosity increase simultaneously. The upper member of the WLBS had a high porosity, low TOC, and high content of clay minerals, thus implying that the interbedded pores of clay minerals contribute to massive pores. Furthermore, porosity was positively correlated with Ro values, in which the Pearson correlation coefficient is 0.7589 (Figure 9b), which indicated that pores in the shale reservoir gradually increased with the advancement of thermal evolution.

Pore Structure
The 3D-FIB images provide a method of visually observing the characteristics of nanopores above 1.0 nm, and were performed for shale samples from the WLBS in the Nanchuan area of the Sichuan Basin. The images showed that the organic nanopores were extremely abundant and had a good connectivity ( Figure 10). Through statistical analysis of more than 4000 organic pores in each sample, the majority of pores were <10 nm in width ( Figure 10). The number of pores >100 nm in width increased significantly in the upper member of the Longmaxi Formation (Figure 10i

Pore Structure
The 3D-FIB images provide a method of visually observing the characteristics of nanopores above 1.0 nm, and were performed for shale samples from the WLBS in the Nanchuan area of the Sichuan Basin. The images showed that the organic nanopores were extremely abundant and had a good connectivity ( Figure 10). Through statistical analysis of more than 4000 organic pores in each sample, the majority of pores were <10 nm in width ( Figure 10). The number of pores >100 nm in width increased significantly in the upper member of the Longmaxi Formation (Figure 10i) in comparison to that of the bottom of the Longmaxi Formation and the Wufeng Formation (Figure 10c,f,i).

Gas Content of Shale
The results of the gas adsorption analysis for samples from Well A revealed that the adsorption capacity of methane (calculated by the Langmuir equation) was between 1.72 m 3 /t and 4.66 m 3 /t (Table 2, Figure 11), which gradually decreased from the bottom upwards ( Figure 3). By contrast, the geological factors of WLBS, e.g., thickness, depth, organic matter, thermal maturity and mineral components, are similar to the Marcellus shale in the Appalachia Basin in North America and lower Cambrian shale (Qiongzhousi Formation and its equivalent shale). Previous research suggested that organic matter played a major role in gas adsorption in shale reservoirs [23,24,35,36]. A large number of na-

Gas Content of Shale
The results of the gas adsorption analysis for samples from Well A revealed that the adsorption capacity of methane (calculated by the Langmuir equation) was between 1.72 m 3 /t and 4.66 m 3 /t (Table 2, Figure 11), which gradually decreased from the bottom upwards ( Figure 3). By contrast, the geological factors of WLBS, e.g., thickness, depth, organic matter, thermal maturity and mineral components, are similar to the Marcellus shale in the Appalachia Basin in North America and lower Cambrian shale (Qiongzhousi Formation and its equivalent shale). Previous research suggested that organic matter played a major role in gas adsorption in shale reservoirs [23,24,35,36]. A large number of nanoscale pores were generated in organic matter, which would provide massive specific surface area for gas adsorption. The shale gas molecules mainly adsorbed on the pore surfaces. The quantities of gas adsorption and the TOC in the WLBS exhibited a clear positive relationship, in which the Pearson correlation coefficient was 0.9471 (Figure 12a), indicating that organic pores in the shale could provide abundant spaces for methane absorption and improve the capacity of gas absorption in the shale reservoir. Through statistical analysis of the gas volume and lost gas volume, the total gas content of the samples was found to be between 0.44 m 3 /t and 5.19 m 3 /t (Table 5), gradually decreasing from the bottom to the top (Figure 3). A positive correlation between the gas content and TOC, in which the Pearson correlation coefficient was 0.7663, indicated that the organic pores provide the main storage space for shale gas in the study area, and the gas content increases sharply in TOC >3.0% (Figure 12b). Therefore, the organic matter content of the WLBS is considered to be the most important factor influencing shale gas accumulation in the study area. increases sharply in TOC >3.0% (Figure 12b). Therefore, the organic matter content of the WLBS is considered to be the most important factor influencing shale gas accumulation in the study area.

Coupling between Source Rock and Reservoir of Shale Gas
As the hydrocarbon source, both the gas potential and the gas amount of shale are determined by the organic matter content of shale [4,5,37,38]. Meanwhile, shale also acts as a reservoir for shale gas [39]; thus, the reservoir capacity of shale is crucial for the enrichment of shale gas, especially the characteristics of the organic pores, which determine the adsorption and preservation of shale gas [37,38]. The WLBS contains massive rigid

Coupling between Source Rock and Reservoir of Shale Gas
As the hydrocarbon source, both the gas potential and the gas amount of shale are determined by the organic matter content of shale [4,5,37,38]. Meanwhile, shale also acts as a reservoir for shale gas [39]; thus, the reservoir capacity of shale is crucial for the enrichment of shale gas, especially the characteristics of the organic pores, which determine the adsorption and preservation of shale gas [37,38]. The WLBS contains massive rigid mineral granules (such as quartz and feldspar) forming intergranular spaces, where organic matters could be stored during the period of hydrocarbon generation. The WLSB in Sichuan Basin has undergone a long history of evolution, resulting in the high thermal maturity of organic matters. It has been proved above that the high content of organic matter in WLBS was favorable for the shale gas accumulation. The WLBS has high thermal maturity due to the high values of Ro, resulted in abundant pores existing in organic matter. The pores in the organic matter of WLBS provide an important adsorbent of absorbed gas and spaces for free gas. For this reason, the degree of organic matter pore development controls the ability to store natural gas. Therefore, the shale in the carbonaceous siliceous/argillaceous deep shelf in the lower member of WLBS with high TOC is considered to have both a strong hydrocarbon generation potential and storage capacity for shale gas, resulting in high gas content. However, the upper member of the WLBS was found to have a low TOC content and thus low gas content, although porosity was determined to be high. Overall, the shale gas would be accumulated under both favorable conditions of source rock and reservoir in the shale.

Conclusions
(1) The most important mineral in Wufeng-Longmaxi Formation is quartz followed by clay minerals, with a small amount of carbonate minerals and feldspar. The shale of Wufeng-Longmaxi Formation in the Sichuan Basin was divided into 5 types of lithofacies (carbonaceous siliceous shale, carbonaceous argillaceous shale, composite shale, silty shale, and argillaceous shale) and 4 types of sedimentary microfacies (carbonaceous siliceous deep-shelf, carbonaceous argillaceous deep-shelf, silty argillaceous shallow-shelf, and argillaceous shallow-shelf).
(2) The values of TOC in Wufeng-Longmaxi Formation basically ranged from 0.5% to 6.0% (about 2.54% on average), and gradually decreased vertically from the bottom to the top, which was controlled by the oxygen content of the bottom water. The organic matter in it was mainly sapropel with high maturity.
(3) The shale reservoir of Wufeng-Longmaxi Formation was found to be characterized by low porosity and low permeability. The types of pore include organic pore, interbedded pore of clay minerals, intergranular pore, intragranular pore, microfractures. The pore types were mainly <10 nm organic pores, especially in the lower member of the Longmaxi Formation. Inorganic pores were observed to increase sharply in the upper member of the Longmaxi Formation.
(4) The volumes of methane adsorption were between 1.431 m 3 /t and 3.719 m 3 /t and the total gas content of samples were distributed between 0.44 m 3 /t and 5.19 m 3 /t, both of which gradually decreased from the bottom upwards. This indicates that lower member of Wufeng-Longmaxi Formation possessed stronger capacity for gas absorption and storage than the upper member.
(5) The pores in the organic matter of the Wufeng-Longmaxi Formation provide important spaces for absorbed gas and free gas. Shale with high TOC content in the carbonaceous siliceous/argillaceous deep-shelf lithofacies is considered to have favorable hydrocarbon generation potential and storage capacity, providing favorable conditions of the source rock and reservoir for shale gas.