Characteristics of Vein-Forming Fluids in the Sinian Dengying Formation Reservoir and Its Relationship with the Hydrocarbon Accumulation Process in the Southwest and Southeast of the Sichuan Basin

Multistage fluid activities and hydrocarbon accumulation processes have occurred in the Dengying Formation of the Sichuan Basin during its long geological history. Petrography and cathodoluminescence observations; in situ microanalysis of rare earth elements, carbon, oxygen, and strontium isotopes; fluid inclusion microthermometric experiments; laser Raman experiments; burial history; thermal history; and hydrocarbon generation history simulation have been applied to study the characteristics of vein-forming fluid in the Dengying Formation reservoirs in the southeast and southwest of Sichuan Basin and to analyze in-depth the multistage fluid activity and hydrocarbon accumulation process. The results show that two stages of dolomite and one stage of quartz are developed in the 4th member of the Dengying Formation in the southeast of Sichuan Basin, and three stages of dolomite are developed in the 2nd member of the Dengying Formation in the southwest of Sichuan Basin. The source of the dolomite veins is mainly reservoir marine diagenetic fluid. Dolomites developed in the Hercynian period were affected by hydrothermal activity to a certain extent which may have been caused by the activity of the Emei mantle plume. The diagenetic mineral sequence of the 4th member of the Dengying Formation in the southeast of Sichuan Basin is quartz (432 Ma)/dolomite I (421 Ma)/dolomite II (288 Ma), and the 2nd member of the Dengying Formation in the southwest of the Sichuan Basin is dolomite I (425 Ma)/dolomite II (283 Ma)/dolomite III (262 Ma). The main hydrocarbon accumulation period was during the Hercynian–Indosinian stage which was related to the thermal influence of the Emei mantle plume activity on the source rock of the Qiongzhusi Formation. Combined with petrography, inclusion thermometry, burial history, and hydrocarbon generation history simulation, the fluid activity and hydrocarbon accumulation evolution sequence in the southeast and southwest of the Sichuan Basin are determined comprehensively.


Introduction
In recent years, with the further progress of petroleum exploration, natural gas resources in the deep strata have become a hot spot in the field of oil and gas exploration [1][2][3][4][5].
In the central area of the Sichuan Basin, the industrial gas resources of the deep Cambrian strata have been discovered which are represented by the Anyue and Moxi gas fields [6][7][8][9][10].

Geological Background
The Sichuan Basin is a large petroleum superposed basin, and many years of oil and gas exploration have shown that it contains rich oil and gas resources [6,[36][37][38]. The study area is located in the high steep fold belt in eastern Sichuan Basin and the middle-low steep fold belt in southern Sichuan Basin [12,39]. The lower assemblage strata with a geological age of approximately 542-419 Ma (from the Sinian to the Silurian systems) in this area have developed several sets of high-quality source-reservoir-caprock assemblages vertically, which have been new targets for natural gas exploration in recent years ( Figure  2) [38,[40][41][42]. The Sinian Dengying Formation, as one of the main reservoirs, has attracted extensive attention. The Sinian Dengying Formation is one of the oldest oil and gas reservoirs in the world. It is characterized by its old age, large burial depth, and long geological history, which leads to its complex petrogenetic evolution process [15,17,43]. From the bottom to top, the Dengying Formation can be divided into four members: the 1st member (Z2dn 1 ), the 2nd member (Z2dn 2 ), the 3rd member (Z2dn 3 ) and the 4th member (Z2dn 4 ). The lithology of Z2dn 1 is mainly dark gray and gray microcrystal dolomite, and algal-laminated dolomite is locally developed. The Z2dn 2 is rich in algae, and the lithology is mainly a light gray thick layer of algal-laminated dolomite, with local powder crystal dolomite. The lithologic color of the Z2dn 3 is relatively shallow, mainly consisting of light gray algallaminated dolomite and powder-microcrystalline dolomite, and a small amount of silicified dolomite or silicalite can be seen locally. The lithology of the Z2dn 4 is mainly a light gray thick-layered powder-fine crystal dolomite and algal dolomite, and the top surface is partially medium-coarse crystal dolomite [14,28,44]. The sedimentary facies of the

Geological Background
The Sichuan Basin is a large petroleum superposed basin, and many years of oil and gas exploration have shown that it contains rich oil and gas resources [6,[36][37][38]. The study area is located in the high steep fold belt in eastern Sichuan Basin and the middle-low steep fold belt in southern Sichuan Basin [12,39]. The lower assemblage strata with a geological age of approximately 542-419 Ma (from the Sinian to the Silurian systems) in this area have developed several sets of high-quality source-reservoir-caprock assemblages vertically, which have been new targets for natural gas exploration in recent years ( Figure 2) [38,[40][41][42]. The Sinian Dengying Formation, as one of the main reservoirs, has attracted extensive attention. The Sinian Dengying Formation is one of the oldest oil and gas reservoirs in the world. It is characterized by its old age, large burial depth, and long geological history, which leads to its complex petrogenetic evolution process [15,17,43]. From the bottom to top, the Dengying Formation can be divided into four members: the 1st member (Z 2 dn 1 ), the 2nd member (Z 2 dn 2 ), the 3rd member (Z 2 dn 3 ) and the 4th member (Z 2 dn 4 ). The lithology of Z 2 dn 1 is mainly dark gray and gray microcrystal dolomite, and algal-laminated dolomite is locally developed. The Z 2 dn 2 is rich in algae, and the lithology is mainly a light gray thick layer of algal-laminated dolomite, with local powder crystal dolomite. The lithologic color of the Z 2 dn 3 is relatively shallow, mainly consisting of light gray algal-laminated dolomite and powder-microcrystalline dolomite, and a small amount of silicified dolomite or silicalite can be seen locally. The lithology of the Z 2 dn 4 is mainly a light gray thick-layered powderfine crystal dolomite and algal dolomite, and the top surface is partially medium-coarse  [14,28,44]. The sedimentary facies of the Dengying Formation are mainly shallow marine carbonate platform facies (mainly intertidal zone and tidal-flat subfacies), which are rich in algal organisms [45,46]. The sedimentary water energy of the Dengying Formation has gradually transferred from the higher energy intertidal zone to the lower energy environment of the lagoon. The changes in the lithology of the Dengying Formation also reflect this transformation of water energy. The Dengying Formation in the south of the Sichuan Basin has undergone complex tectonic evolution [12,39,47], mainly including an uplift and erosion in Late Sinian, a subsidence in Early Paleozoic, an uplift and erosion stage from Late Silurian to Carboniferous, a subsidence from Permian to Late Cretaceous, and a rapid uplift from Late Cretaceous to now. These complex geological tectonic activities resulted in the active formation fluid of the Dengying Formation, and the evolution of the reservoir and the condition of oil and gas preservation conditions have been significantly adjusted and reformed [25]. Dengying Formation are mainly shallow marine carbonate platform facies (mainly intertidal zone and tidal-flat subfacies), which are rich in algal organisms [45,46]. The sedimentary water energy of the Dengying Formation has gradually transferred from the higher energy intertidal zone to the lower energy environment of the lagoon. The changes in the lithology of the Dengying Formation also reflect this transformation of water energy. The Dengying Formation in the south of the Sichuan Basin has undergone complex tectonic evolution [12,39,47], mainly including an uplift and erosion in Late Sinian, a subsidence in Early Paleozoic, an uplift and erosion stage from Late Silurian to Carboniferous, a subsidence from Permian to Late Cretaceous, and a rapid uplift from Late Cretaceous to now. These complex geological tectonic activities resulted in the active formation fluid of the Dengying Formation, and the evolution of the reservoir and the condition of oil and gas preservation conditions have been significantly adjusted and reformed [25].

Samples and Methods
In this study, vein-bearing carbonate rock samples were selected from two wells in the southeast and southwest of the Sichuan Basin, of which 4 vein filling samples from the

Samples and Methods
In this study, vein-bearing carbonate rock samples were selected from two wells in the southeast and southwest of the Sichuan Basin, of which 4 vein filling samples from the 4th member of the Dengying Formation of the Lin 1 well in the southeast of the Sichuan Basin and 3 vein filling samples from the 2nd member of the Dengying Formation of the Jinshi 1 well in the southwest of the Sichuan Basin were selected. One source rock sample of the Qiongzhusi Formation from the Lin 1 well and two source rocks of the Qiongzhusi Formation from the Jinshi 1 well were selected ( Figure 3).  The samples were made into 100 μm thick, double-sided polished microsections and observed under a Leica microscope. The cathodoluminescence analysis was carried out with a CL8200-MK5 cathodoluminescence instrument. The test conditions were 0.3 Pa, the beam voltage was 11 kV, and the beam current was 300 μA. The samples were made into 100 µm thick, double-sided polished microsections and observed under a Leica microscope. The cathodoluminescence analysis was carried out with a CL8200-MK5 cathodoluminescence instrument. The test conditions were 0.3 Pa, the beam voltage was 11 kV, and the beam current was 300 µA.
The temperature of fluid inclusions was measured using double-sided polished microsections with a thickness of 100 µm and the test instrument was a Zeiss Axio Scope. A1 double-channel fluorescence and a transmission light microscope were combined with a LinkAM-THMSG600 hot and cold platform; the error of the hot and cold platform was ±0.1 • C after correction. During temperature measurement process, the heating rate was controlled between 0.1 and~5 • C/min. The inclusion temperatures were observed and recorded when the inclusions were completely homogenized, and the ice was completely melted. The homogenization temperature and freezing point of the brine inclusions were measured.
LA-ICP-MS was used for the microanalysis of the content of elements at the calibration points on the veins. For each point, the diameter of the laser beam spot was 120 µm, the background signal acquisition time was 25 s, and the measurement time was 50 s. The standard sample for the in situ microanalysis of elements was artificial silicate glass NIST610, and the standard sample was re-tested at every 8 points measured. The content of Ca element in the standard sample was taken as the internal standard for the content calculation. The offline processing of the analyzed data was completed by ICPMS-DataCal.
The carbon, oxygen, and strontium isotope tests were conducted at the Key Laboratory of Tectonics and Petroleum Resources, Ministry of Education and State Key Laboratory, China University of Geosciences, Wuhan. The pure carbonate vein samples (dolomite or calcite) separated from the surrounding host rocks were broken into about 200 mesh powder, and reacted with orthophosphoric acid at 25 • C for 1 d to extract carbon dioxide for the carbon and oxygen isotope analyses. The analyses are reported in per mol relative to Vienna Pee Dee Belemnite (V-PDB) for carbon and oxygen with analytical uncertainties of better than ± 0.1‰ (1σ).
A LabRAM HR800 microlaser Raman spectrometer (HORIBA Jobin Yvon S.A.S) was used to conduct the fluid inclusion laser Raman experiment. The test ambient temperature was 25-230 • C, the light source was YAG laser, the wavelength was 532.06 nm, the output power was 350-400 mW, the line width was <0.1 nm, the power of the laser beam on the surface of the sample was generally 60-80 mW, and the confocal effect of the spectrometer could reach the spatial resolution of 0.1 µm in the transverse direction and 0.3 µm in the depth direction. A silicon standard sample with a Raman peak displacement of 520.70 cm −1 was used for wave value correction of the instrument. The time of single data acquisition was generally 10~20 s, and 20~70 times of stacking.
The BasinMod-1D software was used to simulate the burial history, thermal history, and mature hydrocarbon generation history. Based on logging lithology and stratification data, the reciprocal compaction model was used to recover the thickness of strata in different geological periods, and then the burial history was simulated. The BasinMod-1D software default values were used for the initial porosity and compaction factor of pure lithology. By counting the percentage of pure lithology in each layer and calculating the arithmetic average value of each parameter, the assignment of mixed lithology parameters was realized. Based on the burial history and thermal history simulation, the maturation and hydrocarbon generation history of the Qiongzhusi Formation source rock was recovered.

Petrographic Characteristics
The pore, cavity, and fracture of carbonate reservoir in the 4th member of the Sinian Dengying Formation in the Lin 1 well in the southeast of the Sichuan Basin are filled with complex multistage minerals. The veins are mainly filled with carbonate minerals, which are generally filled with multistage dolomite. Some amount of clastic quartz is found within veins ( Figure 3). The veins of the 2nd member of the Dengying Formation in the Jinshi 1 well in the southwest of the Sichuan Basin are mainly distributed in the dissolution cavities ( Figure 3). The overall performance of the veins is similar to that of the Lin 1 well, which are filled with multistage dolomite.
According to the observations of core sample and thin section under microscope, the veins of the reservoir in the 4th member of the Dengying Formation of the Lin 1 well are mainly fracture-cavity filling type. The veins are mostly distributed in the surrounding rock in strips, and the widths of veins are different which are distributed in the range of 1~5 mm (Figure 3). In addition, dolomite and quartz are also found in dissolution pores in core samples. Thin section microscopic observations showed significantly different occurrence developments in the vein body sizes of multistage dolomite ( Figure 4A,C). The cathodoluminescence of the thin section in the Lin 1 well shows that two stages of dolomite (dolomite I and dolomite II) and one stage of quartz are developed in the 4th member of the Dengying Formation. Dolomite I is in contact with the surrounding rock, and the cathodoluminescence color is dark red or close to no luminescence. Dolomite II mineral particles are massive coarse grained and in contact with the first stage dolomite, and the cathodoluminescence color is bright red ( Figure 4A,B). At the same time, quartz and dolomite are filled in the pores under the observation of a thin section ( Figure 4C). The cathodoluminescence shows that quartz does not emit light, the dolomite shines red, and asphalt is filled in the pores between quartz and dolomite ( Figure 4D,E). In addition, dolomite is developed inside the strip quartz vein, the quartz vein is in contact with the surrounding rock, and the dolomite grows and develops in the middle of the quartz. The cathodoluminescence shows that the quartz vein does not emit light, and the dolomite shines red ( Figure 4F Figure 5F). At the same time, liquid oil (asphalt at present) filling can be seen in the pores between the filled coarse-grained dolomite mineral grains ( Figure 5I).

Rare Earth Elements (REEs)
Rare earth elements can be used to classify the formation stages of veins, and the properties and sources of fluids can be inferred from the morphology of rare earth element distribution patterns [48][49][50][51].
The total REE concentration of the Lin 1 well ranges from 0.056 ppm to 0.558 ppm with an average of 0.273 ppm, and the total REE contents in the Jinshi 1 well ranges from 0.022 ppm to 0.825 ppm, with an average value of 0.280 ppm (Table 1). In the REE distribution of the vein body of the Lin 1 well in the southeast of the Sichuan Basin, the LREE/HREE ratio ranges from 0.388 to 0.590, and the average value is 0.509, and in the Jinshi 1 well, the LREE/HREE ratio ranges from 0.965 to 1.352, and the average value is  (Table 1).   banded dolomite, which was deposited in the early syngenetic period and does not emit light under cathodoluminescence ( Figure 5C,E,H). Dolomite Ⅱ and dolomite Ⅲ are coarsegrained dolomites, and Dolomite Ⅱ does not glow under cathodoluminescence, while Dolomite Ⅲ emits red light ( Figure 5C,E,H). Coarse-grained dolomite is found in the outer ring banded algal dolomite in several thin sections ( Figure 5F). At the same time, liquid oil (asphalt at present) filling can be seen in the pores between the filled coarse-grained dolomite mineral grains ( Figure 5I).   the Lin 1 well ranges from 0.457 to 0.747 with an average value of 0.604, and that of the Jinshi 1 well ranges from 0.482 to 0.798 with an average value of 0.584. The rare earth elements in the vein body of the Lin 1 and Jinshi 1 wells present positive Eu anomaly in general ( Figure 6), of which the δEu (δEu = Eu/((Sm + Gd)/2) N, N = normalized value by PAAS) distribution ranges from 0.765 to 1.628 in the Lin 1 well, and the vein body of the Jinshi 1 well also shows positive Eu anomaly with the δEu ranging from 0.894 to 1.753 (Table 1).   Table 2). The values of carbon and oxygen isotopes in dolomite of the 4th member of the Dengying Formation in the Lin 1 well are lower than those of surrounding rock. The carbon and oxygen isotope values of the dolomite in the 2nd member of the Dengying Formation of the Jinshi 1 well show similar characteristics and are lower than those of surrounding rock. However, the carbon and oxygen isotope values of the dolomite in the 4th member of the Dengying Formation in the Lin 1 well are lower than those of the dolomite in the 2nd member of the Dengying Formation in the Jinshi 1 well, showing a negative deviation to a certain extent. The difference between the carbon and oxygen isotope values of the dolomite in the 2nd member of the Dengying Formation in the Jinshi 1 well and the surrounding rock is larger than those between the dolomite in the 4th member of the Dengying Formation in the Lin 1 well and the surrounding rock, and the oxygen isotope values of the dolomite are more negative than those of the surrounding rock. The strontium isotope values of the dolomite in the 4th member of the Dengying Formation in the Lin 1 well are all higher than those of the surrounding rock, and there is little difference between the strontium isotope values of the dolomite in the 2nd member of the Dengying Formation in the Jinshi 1 well and those of surrounding rock, except for one dolomite sample whose strontium isotope values are higher than those of the surrounding rock. The strontium isotope of the dolomite in the 4th member of the Dengying Formation in the Lin 1 well is generally higher than that in the 2nd member of the Dengying Formation in the Jinshi 1 well.

Characteristics of Fluid Inclusions
A large number of fluid inclusions are present in the carbonate reservoir veins of the Dengying Formation in the Lin 1 well in the southeast of the Sichuan Basin and the Jinshi 1 well in the southwest of the Sichuan Basin, which are mainly gas-liquid two-phase brine inclusions (Inclusion I) and a small amount of single-phase methane inclusions (Inclusion II). A small amount of methane-bearing brine inclusions (Inclusion III) is also developed. Methane inclusions have a lens-concentrating effect, which means they appear black at the edge and bright white at the middle when viewed under a transmission light microscope [52,53]. Primary brine inclusions are mainly developed in the dolomite minerals of the Dengying Formation in the Lin 1 well, which are oval and irregular in shape with a long axis size of 6-21 µm. In addition to the primary brine inclusions, a few methane-bearing brine inclusions are also developed ( Figure 7A). Methane inclusions are developed in quartz minerals that are irregular in shape with long axis sizes of 3-8 µm and are associated with brine inclusions (Inclusion I) ( Figure 7C), which were captured in the same period as methane inclusions. The secondary methane inclusions are mostly irregular and elliptical in shape with a linear mass aggregation distribution and a long axis of 4-15 µm ( Figure 7B). A large number of brine inclusions, and a small amount of methane inclusions and methane-bearing brine inclusions are developed in dolomite minerals of the Dengying Formation in the Jinshi 1 well. Most brine inclusions are approximately round or irregular in shape and small in volume, with a long axis size of 3-7 µm ( Figure 7E). Some brine inclusions are linear distribution and are secondary brine inclusions ( Figure 7D), which may have been formed by later fluid charging. The quantity of pure methane inclusions in dolomite minerals of the Dengying Formation in the Jinshi 1 well is small and the shapes of the inclusions are small, with long axis sizes of about 2 µm ( Figure 7F). However, the quantity of methane-bearing brine inclusions in dolomite minerals is large ( Figure 7D). mately round or irregular in shape and small in volume, with a long axis size of 3-7 μm ( Figure 7E). Some brine inclusions are linear distribution and are secondary brine inclusions ( Figure 7D), which may have been formed by later fluid charging. The quantity of pure methane inclusions in dolomite minerals of the Dengying Formation in the Jinshi 1 well is small and the shapes of the inclusions are small, with long axis sizes of about 2 μm ( Figure 7F). However, the quantity of methane-bearing brine inclusions in dolomite minerals is large ( Figure 7D).  mary saline inclusions in the quartz ranges from 121.2 °C to 164.2 °C, and the salinity ranges from 13.9% to 17.8%. The homogenization temperature and salinity of the primary brine inclusions in dolomite Ⅰ and dolomite Ⅱ reservoirs in the 2nd member of the Dengying Formation of the Jinshi 1 well are 112.9~136.7 °C, 9.7~11.9% and 131.5~159.7 °C, 10.7~12.7%, respectively. The homogenization temperature of primary brine inclusions in the dolomite Ⅲ ranges from 153.3 °C to 174.9 °C, and the salinity ranges from 13.1% to 16.2% (Figure 8). Through the analysis of petrographic characteristics of fluid inclusions in reservoir filling mineral particles and the identification of in situ Raman spectrum characteristic peak of fluid inclusions, the composition of fluid inclusions in mineral particles is accurately determined [54,55]. In the 4th member of the Dengying Formation in the Lin 1 well, pure methane gas inclusions ( Figure 9A) and methane-bearing brine inclusions ( Figure  9B) are developed in quartz minerals. The signal intensity of the methane characteristic peak is not obvious at 300 grating, but it is obvious at 1800 grating. The composition of methane-bearing brine inclusions is methane gas and a certain content of water ( Figure  9B). A very small number of pure methane inclusions ( Figure 9C) and a large number of methane-bearing brine inclusions are developed in dolomite minerals of the 2nd member of the Dengying Formation in the Jinshi 1 well. The composition of methane-bearing brine inclusions is methane gas and water with low signal intensity of methane characteristic peak ( Figure 9D). Through the analysis of petrographic characteristics of fluid inclusions in reservoir filling mineral particles and the identification of in situ Raman spectrum characteristic peak of fluid inclusions, the composition of fluid inclusions in mineral particles is accurately determined [54,55]. In the 4th member of the Dengying Formation in the Lin 1 well, pure methane gas inclusions ( Figure 9A) and methane-bearing brine inclusions ( Figure 9B) are developed in quartz minerals. The signal intensity of the methane characteristic peak is not obvious at 300 grating, but it is obvious at 1800 grating. The composition of methanebearing brine inclusions is methane gas and a certain content of water ( Figure 9B). A very small number of pure methane inclusions ( Figure 9C) and a large number of methanebearing brine inclusions are developed in dolomite minerals of the 2nd member of the Dengying Formation in the Jinshi 1 well. The composition of methane-bearing brine inclusions is methane gas and water with low signal intensity of methane characteristic peak ( Figure 9D).

BasinMod Simulates the Stage of Hydrocarbon Accumulation Evolution
The Cambrian Qiongzhusi Formation in the southeast and southwest of the Sichuan Basin is mainly composed of black and gray mudstone and shale, and the organic matter type is sapropelic kerogen. According to the actual situation in the southeast and southwest of the Sichuan Basin, the BasinMod1D software is used to reconstruct the hydrocarbon generation history of the Lin 1 and Jinshi 1 wells. The hydrocarbon generation evolution from the source rock of the Qiongzhusi Formation in the Lin 1 well ( Figure 10A) can be divided into two geological time periods, the first period is 460-400 Ma, and the second period is 300-270 Ma. The first period was the early oil generation stage, accompanied by a small amount of natural gas generation; the second period was the main oil generation stage and gas generation stage, and the oil generation rate reaches a peak about 289 Ma. In the second period, the crude oil previously charged into the reservoir of the Dengying Formation was cracked in situ when the maturity reached and exceeded 2.0%Ro, resulting in a large amount of methane gas formation. The Cambrian Qiongzhusi Formation of the Jinshi 1 well in the southwest of the Sichuan Basin is mainly composed of black and gray mudstone and shale, and the organic matter type is mainly sapropelic kerogen. The hydrocarbon generation evolution of the source rock in the Jinshi 1 well ( Figure 10B) can be divided into two geological time periods, the first period is 430-400 Ma, and the second period is 290-200 Ma. The first period was the early oil generation stage with less oil and gas generation, and the second period was a large oil generation and gas generation stage.

BasinMod Simulates the Stage of Hydrocarbon Accumulation Evolution
The Cambrian Qiongzhusi Formation in the southeast and southwest of the Sichuan Basin is mainly composed of black and gray mudstone and shale, and the organic matter type is sapropelic kerogen. According to the actual situation in the southeast and southwest of the Sichuan Basin, the BasinMod1D software is used to reconstruct the hydrocarbon generation history of the Lin 1 and Jinshi 1 wells. The hydrocarbon generation evolution from the source rock of the Qiongzhusi Formation in the Lin 1 well ( Figure 10A) can be divided into two geological time periods, the first period is 460-400 Ma, and the second period is 300-270 Ma. The first period was the early oil generation stage, accompanied by a small amount of natural gas generation; the second period was the main oil generation stage and gas generation stage, and the oil generation rate reaches a peak about 289 Ma. In the second period, the crude oil previously charged into the reservoir of the Dengying Formation was cracked in situ when the maturity reached and exceeded 2.0%R o , resulting in a large amount of methane gas formation. The Cambrian Qiongzhusi Formation of the Jinshi 1 well in the southwest of the Sichuan Basin is mainly composed of black and gray mudstone and shale, and the organic matter type is mainly sapropelic kerogen. The hydrocarbon generation evolution of the source rock in the Jinshi 1 well ( Figure 10B

Rare Earth Elements Indicate the Characteristics of Dolomite Vein Fluids
The REE geochemistry characteristics of dolomite veins and dolomite filled in the Lin 1 and Jinshi 1 wells of the Dengying Formation represent the characteristics of the dolomite vein fluids, and, to some extent, reflect the source of dolomite vein fluids and the environment of dolomite vein formation [51,[56][57][58]. The dolomite veins of the 4th member of the Dengying Formation in the Lin 1 well are characterized by a relative loss of LREE and relative enrichment of HREE, and they all show obvious negative Ce anomaly characteristics. It shows the characteristics of modern marine carbonate rocks [59,60]. The Y/Ho values also indicate a source of marine fluids [61]. The Dengying Formation is a marine carbonate sedimentary formation, and therefore, the dolomite veins are mainly derived from marine diagenetic fluids of the same layer. The REE distribution curves of dolomite Ⅱ show positive Eu anomaly on the whole ( Figure 6A), indicating that it is affected by hydrothermal activity to a certain extent [62][63][64]. The major positive Eu anomaly of dolomite Ⅱ would be diagnostic of the mixing of marine diagenetic fluids with hydrothermal fluids [59]. The homogenization temperature of primary brine inclusions in dolomite Ⅱ is 170.2-211.6 °C ( Figure 8A), and the burial history shows that the time is in the Middle and Late Permian-Early Triassic period ( Figure 11A), which is the active period of the Emei mantle plume activity (Figure 2) [65][66][67]. During this period, hydrothermal fluids entered dolomite in the carbonate reservoirs, which facilitated the exchange of cations between the rock and the hydrothermal fluids. The dolomite Ⅱ vein-forming fluid influenced by the deep hydrothermal fluid caused by the activity of the Emei mantle plume.
The rare earth elements in the dolomite veins of the 2nd member of the Dengying Formation in the Jinshi 1 well in the southwest of the Sichuan Basin show negative Ce anomaly and high Y/Ho values, indicating the characteristics of marine fluids. The results indicate that the dolomite vein-forming fluids are mainly derived from marine diagenetic fluids in the formation, just as in the Lin 1 well. Dolomite Ⅱ and dolomite Ⅲ show Eu

Rare Earth Elements Indicate the Characteristics of Dolomite Vein Fluids
The REE geochemistry characteristics of dolomite veins and dolomite filled in the Lin 1 and Jinshi 1 wells of the Dengying Formation represent the characteristics of the dolomite vein fluids, and, to some extent, reflect the source of dolomite vein fluids and the environment of dolomite vein formation [51,[56][57][58]. The dolomite veins of the 4th member of the Dengying Formation in the Lin 1 well are characterized by a relative loss of LREE and relative enrichment of HREE, and they all show obvious negative Ce anomaly characteristics. It shows the characteristics of modern marine carbonate rocks [59,60]. The Y/Ho values also indicate a source of marine fluids [61]. The Dengying Formation is a marine carbonate sedimentary formation, and therefore, the dolomite veins are mainly derived from marine diagenetic fluids of the same layer. The REE distribution curves of dolomite II show positive Eu anomaly on the whole ( Figure 6A), indicating that it is affected by hydrothermal activity to a certain extent [62][63][64]. The major positive Eu anomaly of dolomite II would be diagnostic of the mixing of marine diagenetic fluids with hydrothermal fluids [59]. The homogenization temperature of primary brine inclusions in dolomite II is 170.2-211.6 • C ( Figure 8A), and the burial history shows that the time is in the Middle and Late Permian-Early Triassic period ( Figure 11A), which is the active period of the Emei mantle plume activity (Figure 2) [65][66][67]. During this period, hydrothermal fluids entered dolomite in the carbonate reservoirs, which facilitated the exchange of cations between the rock and the hydrothermal fluids. The dolomite II vein-forming fluid influenced by the deep hydrothermal fluid caused by the activity of the Emei mantle plume. marine diagenetic fluid and hydrothermal fluid ( Figure 6B). The homogenization temperatures of primary brine inclusions in the minerals of the dolomite Ⅱ and dolomite Ⅲ in the Jinshi 1 well range from 131.5 °C to 159.7 °C and 153.3 °C to 174.9 °C, respectively, indicating that the age is in the Middle Permian-Triassic period ( Figure 11B), which is also the active period of the Emei mantle plume activity. Therefore, the influence of hydrothermal activity on dolomite comes from the deep hydrothermal activity caused by the Emei mantle plume activity (Figure 2).

Carbon, Oxygen, and Strontium Isotopes Indicate the Characteristics of Dolomite Vein Fluids
The isotopic geochemistry characteristics of dolomite veins can also indicate the source of the fluid [68][69][70]. The results show that the dolomite veins and mineral fluids in the Dengying Formation of the Lin 1 and Jinshi 1 wells are derived from carbonate diagenetic fluids of sedimentary origin ( Figure 12). The δ 18 OPDB values of dolomite filled in the 4th member of the Dengying Formation in the Lin 1 well range from −12.81‰ to −11.75‰, and the surrounding rock is −10.21‰ (Table 2), both of which are highly negative values, indicating that the dolomite may be formed from diagenetic fluid in a diagenetic environment. The δ 13 CPDB ranges from 0.42‰ to 2.46‰, and the surrounding rock is 3.06‰. The δ 13 CPDB values of most marine carbonate rocks are between 4‰ and −4‰, indicating that marine carbonate is the most important carbon source of dolomite filled in the 4th member of the Dengying Formation in the Lin 1 well [70] and the carbon in dolomite veins may mainly come from surrounding rock. The δ 18 OPDB values of dolomite filled in the 2nd member of the Dengying Formation in the Jinshi 1 well range from −10.34‰ to −9.63‰, and the surrounding rock is −5.56‰ (Table 2), both of which are high negative values on the whole. The δ 13 CPDB ranges from 2.66‰ to 2.82‰, and the surrounding rock is 3.70‰, which are similar to the characteristics of the Lin 1 well. It indicates that the carbon in dolomite veins in the 2nd member of the Dengying Formation of the Jinshi 1 well is mainly derived from surrounding rock. The δ 13 CPDB and δ 18 OPDB values of the 2nd member of the Dengying Formation in the Jinshi 1 well are higher than those of the 4th member of the Dengying Formation in the Lin 1 well, probably caused by isotopes fractionation in elevated temperatures.  Figure 6B). The homogenization temperatures of primary brine inclusions in the minerals of the dolomite II and dolomite III in the Jinshi 1 well range from 131.5 • C to 159.7 • C and 153.3 • C to 174.9 • C, respectively, indicating that the age is in the Middle Permian-Triassic period ( Figure 11B), which is also the active period of the Emei mantle plume activity. Therefore, the influence of hydrothermal activity on dolomite comes from the deep hydrothermal activity caused by the Emei mantle plume activity ( Figure 2).

Carbon, Oxygen, and Strontium Isotopes Indicate the Characteristics of Dolomite Vein Fluids
The isotopic geochemistry characteristics of dolomite veins can also indicate the source of the fluid [68][69][70]. The residence time of strontium element in seawater is much longer than the mixing time of seawater, therefore, the isotopic composition of marine strontium element is uniform at any time, worldwide. The 87 Sr/ 86 Sr value of dolomite can basically represent the 87 Sr/ 86 Sr ratio of the original fluid during mineral crystallization and precipitation [27,71]. The 87 Sr/ 86 Sr value of dolomite filled in the 4th member of the Dengying Formation in the Lin 1 well ranges from 0.711359 to 0.714824, and the 87 Sr/ 86 Sr value of surrounding rock is 0.709935 (Table 2), which is significantly higher than the 87 Sr/ 86 Sr value of sea water in the Dengying Formation of the same period, 0.7083. It indicates that the vein forming fluid was influenced by strontium-rich fluid [72], which may be related to the denudation of the 4th member of the Dengying Formation by the Tongwan movement [73,74] in the Sinian period (Figure 2). The Tongwan movement caused the strata of the 4th member of the Dengying Formation to be uplifted to the surface and subjected eluviation of atmospheric fresh water which was the rich strontium of crustal origin fluid. The strontium isotope ratio of the crust derived from the chemical weathering of the old silicon-aluminum rocks in the continental crust into the ocean is relatively high, and the average ratio is estimated to be 0.720 ± 0.005 [75]. Therefore, the strontium isotope value of the dolomite filled in the 4th member of the Dengying Formation in the Lin 1 well is relatively high.

Formation Time of Dolomite Veins and Minerals
The homogenization temperature of brine inclusion captured at the same time with methane inclusion represents the capture temperature of methane inclusion at that time, and the capture temperature of primary brine inclusion captured by mineral growth represents the temperature of mineral formation [76,77]. The formation time of veins and minerals can be determined by temperature projection in the burial history. The homogenization temperature may increase as fluid inclusions trapped in minerals undergo deformation, fluid leakage, and rebalancing. As for fluid inclusions in carbonate minerals, they are more likely to be modified later, and therefore, the minimum homogenization temperature of primary brine inclusions in dolomite and quartz is selected to represent the formation temperature of veins to determine the formation time of minerals and veins [78][79][80]. The results show that the formation time of dolomite Ⅰ in the 4th member of the Dengying Formation in the Lin 1 well is about 421 Ma, the formation time of dolomite Ⅱ is about 288 Ma, the formation time of quartz is about 432 Ma, and the capture time of The residence time of strontium element in seawater is much longer than the mixing time of seawater, therefore, the isotopic composition of marine strontium element is uniform at any time, worldwide. The 87 Sr/ 86 Sr value of dolomite can basically represent the 87 Sr/ 86 Sr ratio of the original fluid during mineral crystallization and precipitation [27,71]. The 87 Sr/ 86 Sr value of dolomite filled in the 4th member of the Dengying Formation in the Lin 1 well ranges from 0.711359 to 0.714824, and the 87 Sr/ 86 Sr value of surrounding rock is 0.709935 (Table 2), which is significantly higher than the 87 Sr/ 86 Sr value of sea water in the Dengying Formation of the same period, 0.7083. It indicates that the vein forming fluid was influenced by strontium-rich fluid [72], which may be related to the denudation of the 4th member of the Dengying Formation by the Tongwan movement [73,74] in the Sinian period ( Figure 2). The Tongwan movement caused the strata of the 4th member of the Dengying Formation to be uplifted to the surface and subjected eluviation of atmospheric fresh water which was the rich strontium of crustal origin fluid. The strontium isotope ratio of the crust derived from the chemical weathering of the old silicon-aluminum rocks in the continental crust into the ocean is relatively high, and the average ratio is estimated to be 0.720 ± 0.005 [75]. Therefore, the strontium isotope value of the dolomite filled in the 4th member of the Dengying Formation in the Lin 1 well is relatively high.

Formation Time of Dolomite Veins and Minerals
The homogenization temperature of brine inclusion captured at the same time with methane inclusion represents the capture temperature of methane inclusion at that time, and the capture temperature of primary brine inclusion captured by mineral growth represents the temperature of mineral formation [76,77]. The formation time of veins and minerals can be determined by temperature projection in the burial history. The homogenization temperature may increase as fluid inclusions trapped in minerals undergo deformation, fluid leakage, and rebalancing. As for fluid inclusions in carbonate minerals, they are more likely to be modified later, and therefore, the minimum homogenization temperature of primary brine inclusions in dolomite and quartz is selected to represent the formation temperature of veins to determine the formation time of minerals and veins [78][79][80]. The  Figure 11B).

Multistage Fluid and Process of Hydrocarbon Accumulation
Based on the study of the hydrocarbon accumulation process of the lower Paleozoic in the southeast of the Sichuan Basin, the hydrocarbon generation evolution stage of the Cambrian source rocks and hydrocarbon charging time of the Dengying Formation in the southeast of the Sichuan Basin are determined. The 4th member of the Dengying formation reservoir in the southeast of the Sichuan Basin started oil charging about 460-400 Ma, and then, denudation resulted in hydrocarbon generation stagnation of source rocks and destruction of paleo reservoirs; about 300-270 Ma, the Cambrian source rocks entered the late oil generation stage, followed by the second oil charging stage; about 270 Ma, the reservoir entered the stage of oil cracking and generating dry gas and asphalt; and since the late Yanshan period, the strata were uplifted and denuded violently, forming faults connected to the surface [12,17], causing a large amount of natural gas to escape, and destroying the gas reservoir. The fluid evolution sequence of the 4th member of the Dengying Formation within the Lin 1 well in the southeast of the Sichuan Basin is as follows: quartz (~432 Ma) → dolomite I (~421 Ma) → oil filling I (460-400 Ma) → dolomite II (~288 Ma) → oil filling II (300-270 Ma) → gas escaping (~75 Ma) ( Figure 11A). The recovery pressure coefficient of secondary methane inclusion captured from quartz of the 4th member of the Dengying Formation in the Lin 1 well is 0.85~1.06, which is a normal pressure and poor preservation condition. The homogenization temperature of brine inclusions associated with the secondary methane inclusions shows that the capture time of methane inclusions is about 20 Ma ( Figure 11A). After the Himalayan uplift tectonism, natural gas was lost and the formation pressure and pressure coefficient decreased, and about 60 Ma, the Dengying Formation reservoir returned to a normal pressure state [81]. The methane inclusions captured by the quartz minerals in the 4th member of the Dengying Formation in the Lin 1 well are secondary methane inclusions, which were captured when the gas reservoir was destroyed, so the formation pressure is a normal pressure.
The reservoir of the 2nd member of the Dengying Formation in the southwest of the Sichuan Basin began the first phase of oil charging about 430-400 Ma, and the subsequent denudation caused the stagnation of hydrocarbon generation in the source rocks and destroyed paleo-oil reservoirs at the same time; about 290 Ma, the Cambrian source rock entered the late oil generation stage, followed by the second stage of oil charging in the reservoir; about 290~230 Ma, the reservoir entered the stage of crude oil cracking into gas, generating dry gas and asphalt. During the Himalayan period, the axis of the Leshan-Longnvsi paleo uplift migrated to the Weiyuan structure, while the strata of the Weiyuan structure uplifted sharply, and the overlying strata suffered severe denudation and formed the largest anticline in the Sichuan Basin, the Weiyuan anticline [82][83][84]. At this time, the Jinshi structure became a secondary anticline in the southwest slope belt of the Weiyuan anticline. The reservoir fluid evolution sequence of the 2nd member of the Dengying Formation in the Jinshi 1 well in the southwest of the Sichuan Basin is as follows: dolomite I (~425 Ma) → oil filling I (430-400 Ma) → dolomite II (~283 Ma) → oil filling II (290-230 Ma) → dolomite III (~262 Ma) → gas escaping (~85 Ma) ( Figure 11B). The methane inclusions and brine inclusions in the same fluid inclusion combination on the surface of dolomite mineral particles are captured at the same time, and the capture time of methane-bearing brine inclusions is about 19 Ma which is the period of stratigraphic uplift and denudation ( Figure 11B). The methane laser Raman peak displacements of methane-bearing brine inclusions that are developed in the dolomite of the Jinshi 1 well are distributed in the range of 2913.44~2914.49 cm −1 . The paleo-pressure recovery shows that it is a normal pressure, indicating that the natural gas is captured in the process of gas reservoir adjustment and escape. This is mainly due to the change in the high point of the Jinshi structure. With the formation of the Weiyuan uplift, the Jinshi structure evolves from a higher position to a low structure position, and the natural gas migrates to the Weiyuan structure [85,86], during which a small amount of natural gas is captured by dolomite under normal pressure.