# Difference of Microfeatures among Diagenetic Facies in Tight Sandstone Reservoirs of the Triassic Yanchang Formation in the Midwestern Region, Ordos Basin

Authors: Jian Shi; Xiaolong Wan; Qichao Xie; Shuxun Zhou; Yan Zhou; Dazhong Ren; Rongjun Zhang
Journal: Mathematical Problems in Engineering
 (2021)

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## Abstract

Based on the background of sedimentary characteristics, a large amount of core and thin section analysis, taking Chang 6 reservoir of Yanchang Formation in the central and western Ordos Basin as an example, through the application of scanning electron microscopy, high-pressure mercury injection, nuclear magnetic resonance and microscopic water drive oil model, and other experimental test methods, the diagenetic facies types and microscopic pore structure characteristics of tight sandstone reservoirs are discussed and analyzed in depth. The results show that the average porosity loss rate caused by early diagenesis compaction in the study area is 50.62%, which is the main reason for reservoir compactness. The cementation further causes porosity loss, and the later dissolution increases the reservoir space in the study area to a certain extent. Different diagenetic facies reservoirs not only have obvious differences in porosity evolution characteristics but also have significant differences in pore throat radius distribution characteristics, movable fluid occurrence characteristics, and water drive oil characteristics. The pore throat distribution with radius greater thanR50∼R60 determines the permeability. The difference in movable fluid saturation mainly depends on the connectivity of the relative large pore space corresponding to the relaxation time greater than the cut-off value of T2. The size of pore throat radius has a good control effect on water flooding efficiency.


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## Body

## 1. Introduction

In recent years, with the decreasing of conventional oil and gas resources, the world has increased the exploration and development of unconventional energy, especially tight oil and gas [1–9]. Compared with conventional sandstone reservoirs, tight sandstone reservoirs are characterized by small pore throats (micro- and nanoscale), complex pore structure, and strong micro- and macroheterogeneity [10]. Among them, the pore microstructure, pore type, pore evolution and control factors, and reservoir performance parameters have become the focus of tight oil reservoir research [11, 12]. The Ordos Basin is an early area of tight oil and gas exploration and development in China. The tight oil and gas resources are very rich and have broad prospects for exploration and development [13–15]. The Ordos Basin is the second largest sedimentary basin in my country. It is structurally located on the western edge of the North China Craton [16, 17]. The internal structure of the basin is relatively simple and the stratum is relatively gentle. The overall appearance is large monoclinic with wide and gentle on the east flank and steep and narrow on the west flank (Figure 1).Figure 1
Geographical location of the midwestern regions, Ordos Basin.During the deposition process of Yanchang Formation in the Ordos Basin, the target reservoir rocks were compacted due to compaction and cementation, and a large number of micro- and nanoscale pore throats developed [18–20]. The types and distribution characteristics of micropore throats restrict the quality and development effect of tight sandstone reservoirs. Due to the different degree of diagenesis, the micropore throat parameters of tight sandstone reservoirs are significantly different. Even if the permeability level is the same, the pore throat parameters and distribution law may also show different characteristics. The complex pore throat structure characteristics lead to the changeable occurrence state and distribution characteristics of fluid in the pore throat, which directly restricts the next exploration and development. Therefore, it is necessary to analyze the microscopic pore structure characteristics under different diagenesis, hoping to provide reference for the optimization of high quality target areas of tight sandstone reservoirs. Based on the auxiliary experimental results of casting thin section, scanning electron microscope, X-ray diffraction, and cathodoluminescence, the microscopic pore structure and seepage characteristics of the study area were studied by high-pressure mercury injection, nuclear magnetic resonance, and microscopic water flooding experiments. The differences of microscopic characteristics of different diagenetic phases were analyzed, and the main influencing factors of microscopic characteristics were clarified, so as to provide guidance for further understanding the heterogeneity of tight sandstone reservoirs and evaluating the effective reservoir distribution.


## 2. Experimental Principle and Sample Information

### 2.1. Pore Throat Structure Test

The mercury injection experiment is one of the important methods to analyze the microscopic pore throat structure of the reservoir. The high-pressure mercury intrusion experiment is based on the Washburn equation by converting the mercury entry or exit pressure and the pore diameter to achieve different pore diameters and mercury entry saturations. The corresponding relationship between the pore size distribution characteristics is further obtained. It is widely used to obtain reservoir microscopic pore structure parameters based on high-pressure mercury intrusion experiments to characterize reservoir quality [21, 22]. The high-pressure mercury intrusion experiment adopts AutoPore IV9510 automatic mercury intrusion instrument from Mike Company, the maximum working pressure of the instrument is 414 MPa, and the measuring range of pore throat radius is 0.003∼1000 μm.


### 2.2. Movable  Fluid Occurrence Test

Place the fluid-containing sample in a static magnetic field, and start to make the hydrogen nuclei contained in the fluid in the rock sample show nuclear magnetic resonance with a suitable radio frequency pulse. Remove the effect of the radio frequency pulse on the rock sample, and the hydrogen nuclei will immediately release energy and appear. For nuclear magnetic resonance signals with a gradual decrease in energy, the time corresponding to this process is the relaxation time [23, 24], and the T2 spectrum curve characteristics of the transverse T2 relaxation time and T2 attenuation are usually used for movable fluid occurrence and pore throat analysis of distribution. Different pore sizes have different corresponding relaxation times. The larger the T2 relaxation time, the larger the pore size, and on the contrary, the smaller the pore. Therefore, the T2 spectrum can be used to reflect the development of the pore radius. Since the pore radius is too small, a large capillary force will obstruct the fluid flow and be constrained. At this time, the corresponding T2 relaxation time is the T2 cut-off value (T2cutcff). The fluid that is less than the cut-off value of T2 is called immovable fluid, and when it is more, it is called movable fluid. Nuclear magnetic resonance T2 spectrum measurement uses RecCore-3000 nuclear magnetic resonance core analyzer, the system frequency is 2∼5 MHz continuously adjustable, the magnetic induction intensity is 0.0940∼0.1175 T, and the frequency accuracy is 0.01 Hz.


### 2.3. Microscopic Water Driving Oil Test

First, the core sample is made into a thin slice model of approximately 2.5cm × 2.5cm × 0.05 cm, and fluids that simulate crude oil and formation water are prepared according to the viscosity of the crude oil and the salinity of formation water in the study area, and dyes are added to dye red and blue, respectively. It is convenient to distinguish under the electron microscope. Make the simulated oil and simulated water flow into the sample model under a certain pressure. Through the use of electron microscope and microscopic image acquisition technology to observe the seepage mode and displacement effect of oil and water in the microscopic pore structure of the sample, it can intuitively reflect the characteristics of oil and water in the microscopic pore structure [25]. This microwater drive oil experiment was mainly implemented at the State Key Laboratory of Continental Dynamics of Northwest University through real sandstone microwater drive experiment equipment.


### 2.4. Sample Information

The tight sandstone reservoirs of the Yanchang Formation in the central and western regions of the Ordos Basin developed delta front subfacies deposits. From the experimental analysis of core physical properties, casting thin sections, scanning electron microscope, and cathodoluminescence of 180 core samples, it is known that the rock types are mainly feldspar sandstone, lithic feldspar sandstone, and feldspar lithic sandstone. Select 10 representative samples from them to further carry out the experimental analysis of high-pressure mercury intrusion, nuclear magnetic resonance, and microscopic water flooding models (Table1).Table 1
Sample information table.
Well numberDepth, mPorosity, %Gas permeability, ×10−3 μm2Experimental testRock typeSedimentary faciesHorizonA1442193.99.390.098Microscopic water driving oil, NMRFeldspar sandstoneDeltaic front subfaciesChang 6H3932247.310.800.253A361945.210.80.137HPMIY1822101.212.30.083A2111922.68.90.058Lithic feldspar sandstoneY1442178.48.40.027H1852226.511.750.085Microscopic water driving oil, NMRH2482037.110.080.023A2962197.610.60.126Feldspar lithic sandstoneChang 8H262199.96.40.016


## 2.1. Pore Throat Structure Test

The mercury injection experiment is one of the important methods to analyze the microscopic pore throat structure of the reservoir. The high-pressure mercury intrusion experiment is based on the Washburn equation by converting the mercury entry or exit pressure and the pore diameter to achieve different pore diameters and mercury entry saturations. The corresponding relationship between the pore size distribution characteristics is further obtained. It is widely used to obtain reservoir microscopic pore structure parameters based on high-pressure mercury intrusion experiments to characterize reservoir quality [21, 22]. The high-pressure mercury intrusion experiment adopts AutoPore IV9510 automatic mercury intrusion instrument from Mike Company, the maximum working pressure of the instrument is 414 MPa, and the measuring range of pore throat radius is 0.003∼1000 μm.


## 2.2. Movable  Fluid Occurrence Test

Place the fluid-containing sample in a static magnetic field, and start to make the hydrogen nuclei contained in the fluid in the rock sample show nuclear magnetic resonance with a suitable radio frequency pulse. Remove the effect of the radio frequency pulse on the rock sample, and the hydrogen nuclei will immediately release energy and appear. For nuclear magnetic resonance signals with a gradual decrease in energy, the time corresponding to this process is the relaxation time [23, 24], and the T2 spectrum curve characteristics of the transverse T2 relaxation time and T2 attenuation are usually used for movable fluid occurrence and pore throat analysis of distribution. Different pore sizes have different corresponding relaxation times. The larger the T2 relaxation time, the larger the pore size, and on the contrary, the smaller the pore. Therefore, the T2 spectrum can be used to reflect the development of the pore radius. Since the pore radius is too small, a large capillary force will obstruct the fluid flow and be constrained. At this time, the corresponding T2 relaxation time is the T2 cut-off value (T2cutcff). The fluid that is less than the cut-off value of T2 is called immovable fluid, and when it is more, it is called movable fluid. Nuclear magnetic resonance T2 spectrum measurement uses RecCore-3000 nuclear magnetic resonance core analyzer, the system frequency is 2∼5 MHz continuously adjustable, the magnetic induction intensity is 0.0940∼0.1175 T, and the frequency accuracy is 0.01 Hz.


## 2.3. Microscopic Water Driving Oil Test

First, the core sample is made into a thin slice model of approximately 2.5cm × 2.5cm × 0.05 cm, and fluids that simulate crude oil and formation water are prepared according to the viscosity of the crude oil and the salinity of formation water in the study area, and dyes are added to dye red and blue, respectively. It is convenient to distinguish under the electron microscope. Make the simulated oil and simulated water flow into the sample model under a certain pressure. Through the use of electron microscope and microscopic image acquisition technology to observe the seepage mode and displacement effect of oil and water in the microscopic pore structure of the sample, it can intuitively reflect the characteristics of oil and water in the microscopic pore structure [25]. This microwater drive oil experiment was mainly implemented at the State Key Laboratory of Continental Dynamics of Northwest University through real sandstone microwater drive experiment equipment.


## 2.4. Sample Information

The tight sandstone reservoirs of the Yanchang Formation in the central and western regions of the Ordos Basin developed delta front subfacies deposits. From the experimental analysis of core physical properties, casting thin sections, scanning electron microscope, and cathodoluminescence of 180 core samples, it is known that the rock types are mainly feldspar sandstone, lithic feldspar sandstone, and feldspar lithic sandstone. Select 10 representative samples from them to further carry out the experimental analysis of high-pressure mercury intrusion, nuclear magnetic resonance, and microscopic water flooding models (Table1).Table 1
Sample information table.
Well numberDepth, mPorosity, %Gas permeability, ×10−3 μm2Experimental testRock typeSedimentary faciesHorizonA1442193.99.390.098Microscopic water driving oil, NMRFeldspar sandstoneDeltaic front subfaciesChang 6H3932247.310.800.253A361945.210.80.137HPMIY1822101.212.30.083A2111922.68.90.058Lithic feldspar sandstoneY1442178.48.40.027H1852226.511.750.085Microscopic water driving oil, NMRH2482037.110.080.023A2962197.610.60.126Feldspar lithic sandstoneChang 8H262199.96.40.016


## 3. Diagenesis Characteristics

### 3.1. Diagenesis Types

#### 3.1.1. Compaction

In the early stage of diagenesis, the loose clastic minerals of the sediments due to the overlying pressure were gradually compacted to close contact. During the process, the pore water was discharged one after another and slowly consolidated into rock. Compaction played an important role after the sand body was deposited. With the deepening of burial, detrital particles often exhibit directional arrangement, close contact relationship, multiple rigid fractures, multiple plastic deformations, etc., and at the same time, a large number of pores are reduced. It will cause great damage to the storage space and seepage capacity of the reservoir, which is an important reason for the deterioration of the reservoir quality. The controlling factors are mainly the pressure of the overlying formation, the ratio of impurity bases, and the compressive resistance of particles [26–28]. Through the observation of thin slices under the microscope, it can be found that the rigid quartz particles exhibit directional arrangement, and the particles are mostly point-line and line contact relationships. In some samples, it can be found that the particles are in concave-convex contact relationship and the phenomenon of particle fracture (Figure 2(a)). Plastic minerals such as plastic cuttings and mica have relatively soft characteristics and are prone to deforming during the compaction process and fill in the particle space, thereby affecting the porosity (Figure 2(b)).Figure 2
Microscope figures of typical diagenetic phenomena of samples.


#### 3.1.2. Cementation

Cementation is the effect of the fluid in the rock consolidating the clastic minerals, causing pore blockage in the process, which is the main reason for the further destruction of the physical properties of the reservoir. The cementation in the study area is more obvious, mainly including authigenic clay minerals, carbonates, and siliceous cements.(1) Clay Mineral Cementation. The formation of clay minerals is mainly determined by the mineral composition, fluid characteristics, and temperature conditions. There are various types of clay minerals in the study area, with high content of chlorite, illite, and kaolinite.Through the microscopic identification, the chlorite in the study area is mainly attached to the surface of the particles in the shape of a crust, which develops in the shape of small sharp flakes or scales (Figure2(c)), and the chlorite is continuously distributed in a film shape (Figure 2(d)). It can not only consolidate the particles, but also have a certain protective effect on the particles and pores. However, a large number of developed chlorites are often easy to fill small pores and even throats, causing physical damage.The illite cementation in the study area is generally developed, mainly in the form of thin film filaments and bridges, which occur in the intergranular pores, often divided into pores and roars, and the overall continuity is poor (Figures2(e) and 2(f)). Illite easily cuts the pore space, thereby reducing the connectivity between each other, causing the pores to become micropores, and the throats are mostly blocked, which reduces the storage performance and seepage capacity of the reservoir to a certain extent.The study area is dominated by authigenic kaolinite, with good crystal shape, mostly in the form of hexagonal plate and vermicular aggregates filled in the pore space (Figure2(g)), which is mostly found in primary intergranular pores and intergranular dissolved pores. Kaolinite cement blocks the pores, resulting in a reduction in pore space and a more complex pore structure. At the same time, the porosity and seepage rate of the reservoir are reduced and the heterogeneity of the reservoir is enhanced. However, kaolinite has more developed intercrystalline pores, which can increase the micropores in the pore space, and it often appears dark brown under thin-film microscope.(2) Carbonate Cementation. Using the statistics of the thin slice experiment data of the sample and the observation under the microscope, it is found that different degrees of carbonate cementation and filling of pores have occurred in the study area. The cementation is dominated by iron calcite (Figure 2(h)). The pores are filled by carbonate, which leads to the loss of a large amount of pore space, and the structure between particles is more complex and diverse.The carbonate in the early diagenesis is mainly calcite in the form of micrite and microcrystalline. When the carbonate ions in the early pore medium reach the saturated state, the early carbonate cement will be precipitated, resulting in a large amount of filling of the pore space. However, calcite filling also improves the ability of sandstone to resist compaction to a certain extent and plays a certain role in the formation of secondary pores for subsequent dissolution. In the middle and late stages, iron ions are often precipitated due to the mutual transformation between rock cuttings and other dark minerals and clay minerals, which are easy to form with the calcite formed in the early stage. The iron calcite is distributed in intergranular pores and dissolved pores (Figure2(i)), making the reservoir rock dense.(3) Silicone Cementation. The siliceous cementation in the study area is mainly manifested by the development of secondary quartz enlargement and authigenic quartz. The secondary enlargement of grade II and III quartz is more common under the microscope, and the edge of the quartz grain is locally developed (Figure 2(j)), and the ring edge is rare. Its formation is mainly related to the mutual transformation of clay minerals and the dissolution of silicate minerals and is controlled by the size of the growth space. It is more common in sandstone reservoirs with small interstitial content. The development of secondary enlarged edges occupies part of the intergranular pore space, which is not conducive to the preservation of intergranular pores. In addition, under the scanning electron microscope, it can be seen that the quartz particles surrounded by the chlorite film have enlarged quartz edges where the local chlorite film is not developed. The authigenic quartz crystals are often filled in the residual intergranular pores.


#### 3.1.3. Corrosion

According to the casting thin section of the sample and the statistics of the experimental data of the scanning electron microscope and the observation under the microscope, the dissolution in the study area is mainly the dissolution of feldspar (0.78%), followed by the dissolution of cuttings (0.13%). The total content of dissolved pores accounts for 28.6% of the total porosity, which improves the reservoir performance and pore-throat connectivity to a certain extent. Feldspar is dissolved to produce secondary dissolution pores (Figure2(k)), which often dissolve along the joint surface (Figure 2(l)). Some feldspars may disappear due to the excessively strong dissolution degree, and the dissolution of lithic debris can be seen locally.


### 3.2. Evolution Characteristics of Porosity

#### 3.2.1. The Influence of Diagenesis on Porosity

Quantitative analysis of compaction is carried out by calculation of porosity after porosity. After compaction, the remaining porosity can be used for the current cement content, intergranular pore content, micropore content, measured porosity, and the total displayed under the thin-film microscope. The correlation between the porosity contents is brought into formulas (i)–(iii) in Table2, and the porosity after compaction can be calculated. According to the contact relationship between particles and cement observed under the microscope, it can help to divide the sequence of the development of different cements, and start to develop with strong dissolution as the boundary, and divide the cement into early and midlate. In the early stage, it was mainly thin-film chlorite, grade I quartz secondary enlargement, calcite, and other cements. In the middle and late stages, it was mainly grade II∼III quartz ring enlargement edge, pom-shaped chlorite, kaolinite, iron calcite, illite, etc. Putting the relevant volume fraction into formulas (iv) and (v) in Table 2, the lost porosity and porosity of the early cementation and the middle and late cementation can be obtained, respectively. The increase in porosity and porosity increase rate due to dissolution are given in formulas (vi) and (vii) in Table 2.Table 2
Quantitative calculation method of sandstone porosity evolution.
Porosity evolution parameterFormulaRemarksInitial porosityΦ1=20.91+22.9/Sd (i)Φ1 represents the original porosity of the unconsolidated sandstone, %; Sd represents the Trask sorting coefficient, Sd = (P25/P75)1/2 (in which P25 and P75 represent the corresponding granular diameter of 25%-in-content particles and 75%-in-content particles in the accumulative granularity curve, respectively, mm)Porosity after compactionΦ2=C+P1+P2×P3/P4 (ii)Fa=Φ1−Φ2/Φ1 (iii)Φ2 represents the porosity after compaction, %; C represents the cement content, %; P1 represents the surface porosity of intergranular pores, %; P2 represents the surface porosity of original micropores, %; P3 represents the measured porosity of the sample, %; P4 represents the total surface porosity, %; Pa represents the porosity loss due to compaction, %; Fa represents the ratio of porosity loss due to compaction, %Porosity after cementationΦ3=Φ2−C (iv)Fb=Φ2−Φ3×100%/Φ1 (v)Φ3 represents the porosity after compaction and cementation, %; Fb represents the ratio of porosity loss due to cementation, %Dissolution increases porosityΦ4=P5×P3/P4 (vi)Fc=Φ4×100%/Φ1 (vii)Φ4 represents the increased porosity due to dissolution, %; P5 represents the total dissolution pore surface area, %; Fc represents the ratio of porosity loss due to dissolution, %The calculation results show (Table3) that the sorting coefficient is mainly distributed between 1.11 and 1.73, with an average of 1.43, which is biased towards fineness. The main distribution range of the initial porosity is 32.96%∼39.68%, with an average of 36.92%, showing a nearly normal distribution, slightly biased towards the roughness. The remaining porosity after compaction in the early diagenesis is mainly distributed between 10.23% and 30.14%, with an average of 18.51%, and the porosity loss rate is between 30.22% and 73.83%, with an average of 50.62%. The remaining porosity distribution ranges from 3.39% to 10.52% after cementation, with an average of 8.13%. The porosity loss caused by early cementation and metasomatism ranges from 1.13% to 14.72%, with an average of 3.96%. The porosity distribution of the middle and late cementation loss ranges from 2.25% to 13.1%, with an average of 6.42%. The secondary dissolution porosity produced by dissolution is 0.34∼7.47%, with an average of 2.26%. It shows that when the pore volume of the reservoir is greatly reduced, the dissolved pores increase the storage space of the reservoir in the study area to a certain extent. However, the wider distribution range has strong uneven characteristics.Table 3
Statistics of porosity evolution in diagenesis.
CompactionInitial porosity, %Porosity after compaction, %The ratio of porosity loss due to compaction, %RangeAverageRangeAverageRangeAverage32.96∼39.6836.8710.23∼30.1418.4330.22∼73.8350.54CementationPorosity loss due to early cementation, %Porosity loss due to the midlate cementation, %Porosity after compaction and cementation, %RangeAverageRangeAverageRangeAverage1.13∼14.723.962.25∼13.16.423.39∼10.528.19CorrosionIncreased porosity due to dissolution, %Final calculation of porosity, %Porosity measured by gas, %Error, %RangeAverageRangeAverageRangeAverageRangeAverage0.34∼7.472.214.82∼13.8710.334.35∼16.7710.750.79∼20.36.89


#### 3.2.2. Porosity Evolution Differences of Different Types of Diagenetic Facies

On the basis of thin section observation and identification data analysis and statistics, by analyzing the response correlation between different mineral characteristics, pore types and distribution characteristics, and macro- and microcharacteristics, the main control minerals, pore types, and other characteristics are shown. Four types of diagenetic facies are divided: the residual chlorite-membrane intergranular-pore diagenetic facies, the feldspar dissolution diagenetic facies, the clay mineral cemented microporous diagenetic facies, and the carbonate cemented tight diagenetic facies (Figure3).Figure 3
Pore evolution process of different diagenetic facies.Formulas (i)∼(vii) in Table2 are used to establish the porosity evolution simulation equations of four different diagenetic facies in the study area. Through the above studies, it is found that, according to the diagenetic evolution process, a large number of minerals and fluids continue to resist compaction, fill pores, and dissolve particles in the pore space of sediments. However, the effects of different diagenesis in different regions and environments are also different, which can be proved by the porosity evolution characteristics of diagenetic facies. The final calculated porosity of residual chlorite-membrane intergranular-pore diagenetic facies is 12.28%. The dissolution porosity of feldspar dissolution diagenetic facies increased the most, with an average of 3.95%. Clay mineral cemented microporous diagenetic facies lost the most porosity due to the middle and late cementation, with an average of 8.11%. The compaction of carbonate cemented tight diagenetic facies leads to the smallest loss of porosity, while the early cementation leads to the largest loss of porosity, which is 17.12%.


## 3.1. Diagenesis Types

### 3.1.1. Compaction

In the early stage of diagenesis, the loose clastic minerals of the sediments due to the overlying pressure were gradually compacted to close contact. During the process, the pore water was discharged one after another and slowly consolidated into rock. Compaction played an important role after the sand body was deposited. With the deepening of burial, detrital particles often exhibit directional arrangement, close contact relationship, multiple rigid fractures, multiple plastic deformations, etc., and at the same time, a large number of pores are reduced. It will cause great damage to the storage space and seepage capacity of the reservoir, which is an important reason for the deterioration of the reservoir quality. The controlling factors are mainly the pressure of the overlying formation, the ratio of impurity bases, and the compressive resistance of particles [26–28]. Through the observation of thin slices under the microscope, it can be found that the rigid quartz particles exhibit directional arrangement, and the particles are mostly point-line and line contact relationships. In some samples, it can be found that the particles are in concave-convex contact relationship and the phenomenon of particle fracture (Figure 2(a)). Plastic minerals such as plastic cuttings and mica have relatively soft characteristics and are prone to deforming during the compaction process and fill in the particle space, thereby affecting the porosity (Figure 2(b)).Figure 2
Microscope figures of typical diagenetic phenomena of samples.


### 3.1.2. Cementation

Cementation is the effect of the fluid in the rock consolidating the clastic minerals, causing pore blockage in the process, which is the main reason for the further destruction of the physical properties of the reservoir. The cementation in the study area is more obvious, mainly including authigenic clay minerals, carbonates, and siliceous cements.(1) Clay Mineral Cementation. The formation of clay minerals is mainly determined by the mineral composition, fluid characteristics, and temperature conditions. There are various types of clay minerals in the study area, with high content of chlorite, illite, and kaolinite.Through the microscopic identification, the chlorite in the study area is mainly attached to the surface of the particles in the shape of a crust, which develops in the shape of small sharp flakes or scales (Figure2(c)), and the chlorite is continuously distributed in a film shape (Figure 2(d)). It can not only consolidate the particles, but also have a certain protective effect on the particles and pores. However, a large number of developed chlorites are often easy to fill small pores and even throats, causing physical damage.The illite cementation in the study area is generally developed, mainly in the form of thin film filaments and bridges, which occur in the intergranular pores, often divided into pores and roars, and the overall continuity is poor (Figures2(e) and 2(f)). Illite easily cuts the pore space, thereby reducing the connectivity between each other, causing the pores to become micropores, and the throats are mostly blocked, which reduces the storage performance and seepage capacity of the reservoir to a certain extent.The study area is dominated by authigenic kaolinite, with good crystal shape, mostly in the form of hexagonal plate and vermicular aggregates filled in the pore space (Figure2(g)), which is mostly found in primary intergranular pores and intergranular dissolved pores. Kaolinite cement blocks the pores, resulting in a reduction in pore space and a more complex pore structure. At the same time, the porosity and seepage rate of the reservoir are reduced and the heterogeneity of the reservoir is enhanced. However, kaolinite has more developed intercrystalline pores, which can increase the micropores in the pore space, and it often appears dark brown under thin-film microscope.(2) Carbonate Cementation. Using the statistics of the thin slice experiment data of the sample and the observation under the microscope, it is found that different degrees of carbonate cementation and filling of pores have occurred in the study area. The cementation is dominated by iron calcite (Figure 2(h)). The pores are filled by carbonate, which leads to the loss of a large amount of pore space, and the structure between particles is more complex and diverse.The carbonate in the early diagenesis is mainly calcite in the form of micrite and microcrystalline. When the carbonate ions in the early pore medium reach the saturated state, the early carbonate cement will be precipitated, resulting in a large amount of filling of the pore space. However, calcite filling also improves the ability of sandstone to resist compaction to a certain extent and plays a certain role in the formation of secondary pores for subsequent dissolution. In the middle and late stages, iron ions are often precipitated due to the mutual transformation between rock cuttings and other dark minerals and clay minerals, which are easy to form with the calcite formed in the early stage. The iron calcite is distributed in intergranular pores and dissolved pores (Figure2(i)), making the reservoir rock dense.(3) Silicone Cementation. The siliceous cementation in the study area is mainly manifested by the development of secondary quartz enlargement and authigenic quartz. The secondary enlargement of grade II and III quartz is more common under the microscope, and the edge of the quartz grain is locally developed (Figure 2(j)), and the ring edge is rare. Its formation is mainly related to the mutual transformation of clay minerals and the dissolution of silicate minerals and is controlled by the size of the growth space. It is more common in sandstone reservoirs with small interstitial content. The development of secondary enlarged edges occupies part of the intergranular pore space, which is not conducive to the preservation of intergranular pores. In addition, under the scanning electron microscope, it can be seen that the quartz particles surrounded by the chlorite film have enlarged quartz edges where the local chlorite film is not developed. The authigenic quartz crystals are often filled in the residual intergranular pores.


### 3.1.3. Corrosion

According to the casting thin section of the sample and the statistics of the experimental data of the scanning electron microscope and the observation under the microscope, the dissolution in the study area is mainly the dissolution of feldspar (0.78%), followed by the dissolution of cuttings (0.13%). The total content of dissolved pores accounts for 28.6% of the total porosity, which improves the reservoir performance and pore-throat connectivity to a certain extent. Feldspar is dissolved to produce secondary dissolution pores (Figure2(k)), which often dissolve along the joint surface (Figure 2(l)). Some feldspars may disappear due to the excessively strong dissolution degree, and the dissolution of lithic debris can be seen locally.


## 3.1.1. Compaction

In the early stage of diagenesis, the loose clastic minerals of the sediments due to the overlying pressure were gradually compacted to close contact. During the process, the pore water was discharged one after another and slowly consolidated into rock. Compaction played an important role after the sand body was deposited. With the deepening of burial, detrital particles often exhibit directional arrangement, close contact relationship, multiple rigid fractures, multiple plastic deformations, etc., and at the same time, a large number of pores are reduced. It will cause great damage to the storage space and seepage capacity of the reservoir, which is an important reason for the deterioration of the reservoir quality. The controlling factors are mainly the pressure of the overlying formation, the ratio of impurity bases, and the compressive resistance of particles [26–28]. Through the observation of thin slices under the microscope, it can be found that the rigid quartz particles exhibit directional arrangement, and the particles are mostly point-line and line contact relationships. In some samples, it can be found that the particles are in concave-convex contact relationship and the phenomenon of particle fracture (Figure 2(a)). Plastic minerals such as plastic cuttings and mica have relatively soft characteristics and are prone to deforming during the compaction process and fill in the particle space, thereby affecting the porosity (Figure 2(b)).Figure 2
Microscope figures of typical diagenetic phenomena of samples.


## 3.1.2. Cementation

Cementation is the effect of the fluid in the rock consolidating the clastic minerals, causing pore blockage in the process, which is the main reason for the further destruction of the physical properties of the reservoir. The cementation in the study area is more obvious, mainly including authigenic clay minerals, carbonates, and siliceous cements.(1) Clay Mineral Cementation. The formation of clay minerals is mainly determined by the mineral composition, fluid characteristics, and temperature conditions. There are various types of clay minerals in the study area, with high content of chlorite, illite, and kaolinite.Through the microscopic identification, the chlorite in the study area is mainly attached to the surface of the particles in the shape of a crust, which develops in the shape of small sharp flakes or scales (Figure2(c)), and the chlorite is continuously distributed in a film shape (Figure 2(d)). It can not only consolidate the particles, but also have a certain protective effect on the particles and pores. However, a large number of developed chlorites are often easy to fill small pores and even throats, causing physical damage.The illite cementation in the study area is generally developed, mainly in the form of thin film filaments and bridges, which occur in the intergranular pores, often divided into pores and roars, and the overall continuity is poor (Figures2(e) and 2(f)). Illite easily cuts the pore space, thereby reducing the connectivity between each other, causing the pores to become micropores, and the throats are mostly blocked, which reduces the storage performance and seepage capacity of the reservoir to a certain extent.The study area is dominated by authigenic kaolinite, with good crystal shape, mostly in the form of hexagonal plate and vermicular aggregates filled in the pore space (Figure2(g)), which is mostly found in primary intergranular pores and intergranular dissolved pores. Kaolinite cement blocks the pores, resulting in a reduction in pore space and a more complex pore structure. At the same time, the porosity and seepage rate of the reservoir are reduced and the heterogeneity of the reservoir is enhanced. However, kaolinite has more developed intercrystalline pores, which can increase the micropores in the pore space, and it often appears dark brown under thin-film microscope.(2) Carbonate Cementation. Using the statistics of the thin slice experiment data of the sample and the observation under the microscope, it is found that different degrees of carbonate cementation and filling of pores have occurred in the study area. The cementation is dominated by iron calcite (Figure 2(h)). The pores are filled by carbonate, which leads to the loss of a large amount of pore space, and the structure between particles is more complex and diverse.The carbonate in the early diagenesis is mainly calcite in the form of micrite and microcrystalline. When the carbonate ions in the early pore medium reach the saturated state, the early carbonate cement will be precipitated, resulting in a large amount of filling of the pore space. However, calcite filling also improves the ability of sandstone to resist compaction to a certain extent and plays a certain role in the formation of secondary pores for subsequent dissolution. In the middle and late stages, iron ions are often precipitated due to the mutual transformation between rock cuttings and other dark minerals and clay minerals, which are easy to form with the calcite formed in the early stage. The iron calcite is distributed in intergranular pores and dissolved pores (Figure2(i)), making the reservoir rock dense.(3) Silicone Cementation. The siliceous cementation in the study area is mainly manifested by the development of secondary quartz enlargement and authigenic quartz. The secondary enlargement of grade II and III quartz is more common under the microscope, and the edge of the quartz grain is locally developed (Figure 2(j)), and the ring edge is rare. Its formation is mainly related to the mutual transformation of clay minerals and the dissolution of silicate minerals and is controlled by the size of the growth space. It is more common in sandstone reservoirs with small interstitial content. The development of secondary enlarged edges occupies part of the intergranular pore space, which is not conducive to the preservation of intergranular pores. In addition, under the scanning electron microscope, it can be seen that the quartz particles surrounded by the chlorite film have enlarged quartz edges where the local chlorite film is not developed. The authigenic quartz crystals are often filled in the residual intergranular pores.


## 3.1.3. Corrosion

According to the casting thin section of the sample and the statistics of the experimental data of the scanning electron microscope and the observation under the microscope, the dissolution in the study area is mainly the dissolution of feldspar (0.78%), followed by the dissolution of cuttings (0.13%). The total content of dissolved pores accounts for 28.6% of the total porosity, which improves the reservoir performance and pore-throat connectivity to a certain extent. Feldspar is dissolved to produce secondary dissolution pores (Figure2(k)), which often dissolve along the joint surface (Figure 2(l)). Some feldspars may disappear due to the excessively strong dissolution degree, and the dissolution of lithic debris can be seen locally.


## 3.2. Evolution Characteristics of Porosity

### 3.2.1. The Influence of Diagenesis on Porosity

Quantitative analysis of compaction is carried out by calculation of porosity after porosity. After compaction, the remaining porosity can be used for the current cement content, intergranular pore content, micropore content, measured porosity, and the total displayed under the thin-film microscope. The correlation between the porosity contents is brought into formulas (i)–(iii) in Table2, and the porosity after compaction can be calculated. According to the contact relationship between particles and cement observed under the microscope, it can help to divide the sequence of the development of different cements, and start to develop with strong dissolution as the boundary, and divide the cement into early and midlate. In the early stage, it was mainly thin-film chlorite, grade I quartz secondary enlargement, calcite, and other cements. In the middle and late stages, it was mainly grade II∼III quartz ring enlargement edge, pom-shaped chlorite, kaolinite, iron calcite, illite, etc. Putting the relevant volume fraction into formulas (iv) and (v) in Table 2, the lost porosity and porosity of the early cementation and the middle and late cementation can be obtained, respectively. The increase in porosity and porosity increase rate due to dissolution are given in formulas (vi) and (vii) in Table 2.Table 2
Quantitative calculation method of sandstone porosity evolution.
Porosity evolution parameterFormulaRemarksInitial porosityΦ1=20.91+22.9/Sd (i)Φ1 represents the original porosity of the unconsolidated sandstone, %; Sd represents the Trask sorting coefficient, Sd = (P25/P75)1/2 (in which P25 and P75 represent the corresponding granular diameter of 25%-in-content particles and 75%-in-content particles in the accumulative granularity curve, respectively, mm)Porosity after compactionΦ2=C+P1+P2×P3/P4 (ii)Fa=Φ1−Φ2/Φ1 (iii)Φ2 represents the porosity after compaction, %; C represents the cement content, %; P1 represents the surface porosity of intergranular pores, %; P2 represents the surface porosity of original micropores, %; P3 represents the measured porosity of the sample, %; P4 represents the total surface porosity, %; Pa represents the porosity loss due to compaction, %; Fa represents the ratio of porosity loss due to compaction, %Porosity after cementationΦ3=Φ2−C (iv)Fb=Φ2−Φ3×100%/Φ1 (v)Φ3 represents the porosity after compaction and cementation, %; Fb represents the ratio of porosity loss due to cementation, %Dissolution increases porosityΦ4=P5×P3/P4 (vi)Fc=Φ4×100%/Φ1 (vii)Φ4 represents the increased porosity due to dissolution, %; P5 represents the total dissolution pore surface area, %; Fc represents the ratio of porosity loss due to dissolution, %The calculation results show (Table3) that the sorting coefficient is mainly distributed between 1.11 and 1.73, with an average of 1.43, which is biased towards fineness. The main distribution range of the initial porosity is 32.96%∼39.68%, with an average of 36.92%, showing a nearly normal distribution, slightly biased towards the roughness. The remaining porosity after compaction in the early diagenesis is mainly distributed between 10.23% and 30.14%, with an average of 18.51%, and the porosity loss rate is between 30.22% and 73.83%, with an average of 50.62%. The remaining porosity distribution ranges from 3.39% to 10.52% after cementation, with an average of 8.13%. The porosity loss caused by early cementation and metasomatism ranges from 1.13% to 14.72%, with an average of 3.96%. The porosity distribution of the middle and late cementation loss ranges from 2.25% to 13.1%, with an average of 6.42%. The secondary dissolution porosity produced by dissolution is 0.34∼7.47%, with an average of 2.26%. It shows that when the pore volume of the reservoir is greatly reduced, the dissolved pores increase the storage space of the reservoir in the study area to a certain extent. However, the wider distribution range has strong uneven characteristics.Table 3
Statistics of porosity evolution in diagenesis.
CompactionInitial porosity, %Porosity after compaction, %The ratio of porosity loss due to compaction, %RangeAverageRangeAverageRangeAverage32.96∼39.6836.8710.23∼30.1418.4330.22∼73.8350.54CementationPorosity loss due to early cementation, %Porosity loss due to the midlate cementation, %Porosity after compaction and cementation, %RangeAverageRangeAverageRangeAverage1.13∼14.723.962.25∼13.16.423.39∼10.528.19CorrosionIncreased porosity due to dissolution, %Final calculation of porosity, %Porosity measured by gas, %Error, %RangeAverageRangeAverageRangeAverageRangeAverage0.34∼7.472.214.82∼13.8710.334.35∼16.7710.750.79∼20.36.89


### 3.2.2. Porosity Evolution Differences of Different Types of Diagenetic Facies

On the basis of thin section observation and identification data analysis and statistics, by analyzing the response correlation between different mineral characteristics, pore types and distribution characteristics, and macro- and microcharacteristics, the main control minerals, pore types, and other characteristics are shown. Four types of diagenetic facies are divided: the residual chlorite-membrane intergranular-pore diagenetic facies, the feldspar dissolution diagenetic facies, the clay mineral cemented microporous diagenetic facies, and the carbonate cemented tight diagenetic facies (Figure3).Figure 3
Pore evolution process of different diagenetic facies.Formulas (i)∼(vii) in Table2 are used to establish the porosity evolution simulation equations of four different diagenetic facies in the study area. Through the above studies, it is found that, according to the diagenetic evolution process, a large number of minerals and fluids continue to resist compaction, fill pores, and dissolve particles in the pore space of sediments. However, the effects of different diagenesis in different regions and environments are also different, which can be proved by the porosity evolution characteristics of diagenetic facies. The final calculated porosity of residual chlorite-membrane intergranular-pore diagenetic facies is 12.28%. The dissolution porosity of feldspar dissolution diagenetic facies increased the most, with an average of 3.95%. Clay mineral cemented microporous diagenetic facies lost the most porosity due to the middle and late cementation, with an average of 8.11%. The compaction of carbonate cemented tight diagenetic facies leads to the smallest loss of porosity, while the early cementation leads to the largest loss of porosity, which is 17.12%.


## 3.2.1. The Influence of Diagenesis on Porosity

Quantitative analysis of compaction is carried out by calculation of porosity after porosity. After compaction, the remaining porosity can be used for the current cement content, intergranular pore content, micropore content, measured porosity, and the total displayed under the thin-film microscope. The correlation between the porosity contents is brought into formulas (i)–(iii) in Table2, and the porosity after compaction can be calculated. According to the contact relationship between particles and cement observed under the microscope, it can help to divide the sequence of the development of different cements, and start to develop with strong dissolution as the boundary, and divide the cement into early and midlate. In the early stage, it was mainly thin-film chlorite, grade I quartz secondary enlargement, calcite, and other cements. In the middle and late stages, it was mainly grade II∼III quartz ring enlargement edge, pom-shaped chlorite, kaolinite, iron calcite, illite, etc. Putting the relevant volume fraction into formulas (iv) and (v) in Table 2, the lost porosity and porosity of the early cementation and the middle and late cementation can be obtained, respectively. The increase in porosity and porosity increase rate due to dissolution are given in formulas (vi) and (vii) in Table 2.Table 2
Quantitative calculation method of sandstone porosity evolution.
Porosity evolution parameterFormulaRemarksInitial porosityΦ1=20.91+22.9/Sd (i)Φ1 represents the original porosity of the unconsolidated sandstone, %; Sd represents the Trask sorting coefficient, Sd = (P25/P75)1/2 (in which P25 and P75 represent the corresponding granular diameter of 25%-in-content particles and 75%-in-content particles in the accumulative granularity curve, respectively, mm)Porosity after compactionΦ2=C+P1+P2×P3/P4 (ii)Fa=Φ1−Φ2/Φ1 (iii)Φ2 represents the porosity after compaction, %; C represents the cement content, %; P1 represents the surface porosity of intergranular pores, %; P2 represents the surface porosity of original micropores, %; P3 represents the measured porosity of the sample, %; P4 represents the total surface porosity, %; Pa represents the porosity loss due to compaction, %; Fa represents the ratio of porosity loss due to compaction, %Porosity after cementationΦ3=Φ2−C (iv)Fb=Φ2−Φ3×100%/Φ1 (v)Φ3 represents the porosity after compaction and cementation, %; Fb represents the ratio of porosity loss due to cementation, %Dissolution increases porosityΦ4=P5×P3/P4 (vi)Fc=Φ4×100%/Φ1 (vii)Φ4 represents the increased porosity due to dissolution, %; P5 represents the total dissolution pore surface area, %; Fc represents the ratio of porosity loss due to dissolution, %The calculation results show (Table3) that the sorting coefficient is mainly distributed between 1.11 and 1.73, with an average of 1.43, which is biased towards fineness. The main distribution range of the initial porosity is 32.96%∼39.68%, with an average of 36.92%, showing a nearly normal distribution, slightly biased towards the roughness. The remaining porosity after compaction in the early diagenesis is mainly distributed between 10.23% and 30.14%, with an average of 18.51%, and the porosity loss rate is between 30.22% and 73.83%, with an average of 50.62%. The remaining porosity distribution ranges from 3.39% to 10.52% after cementation, with an average of 8.13%. The porosity loss caused by early cementation and metasomatism ranges from 1.13% to 14.72%, with an average of 3.96%. The porosity distribution of the middle and late cementation loss ranges from 2.25% to 13.1%, with an average of 6.42%. The secondary dissolution porosity produced by dissolution is 0.34∼7.47%, with an average of 2.26%. It shows that when the pore volume of the reservoir is greatly reduced, the dissolved pores increase the storage space of the reservoir in the study area to a certain extent. However, the wider distribution range has strong uneven characteristics.Table 3
Statistics of porosity evolution in diagenesis.
CompactionInitial porosity, %Porosity after compaction, %The ratio of porosity loss due to compaction, %RangeAverageRangeAverageRangeAverage32.96∼39.6836.8710.23∼30.1418.4330.22∼73.8350.54CementationPorosity loss due to early cementation, %Porosity loss due to the midlate cementation, %Porosity after compaction and cementation, %RangeAverageRangeAverageRangeAverage1.13∼14.723.962.25∼13.16.423.39∼10.528.19CorrosionIncreased porosity due to dissolution, %Final calculation of porosity, %Porosity measured by gas, %Error, %RangeAverageRangeAverageRangeAverageRangeAverage0.34∼7.472.214.82∼13.8710.334.35∼16.7710.750.79∼20.36.89


## 3.2.2. Porosity Evolution Differences of Different Types of Diagenetic Facies

On the basis of thin section observation and identification data analysis and statistics, by analyzing the response correlation between different mineral characteristics, pore types and distribution characteristics, and macro- and microcharacteristics, the main control minerals, pore types, and other characteristics are shown. Four types of diagenetic facies are divided: the residual chlorite-membrane intergranular-pore diagenetic facies, the feldspar dissolution diagenetic facies, the clay mineral cemented microporous diagenetic facies, and the carbonate cemented tight diagenetic facies (Figure3).Figure 3
Pore evolution process of different diagenetic facies.Formulas (i)∼(vii) in Table2 are used to establish the porosity evolution simulation equations of four different diagenetic facies in the study area. Through the above studies, it is found that, according to the diagenetic evolution process, a large number of minerals and fluids continue to resist compaction, fill pores, and dissolve particles in the pore space of sediments. However, the effects of different diagenesis in different regions and environments are also different, which can be proved by the porosity evolution characteristics of diagenetic facies. The final calculated porosity of residual chlorite-membrane intergranular-pore diagenetic facies is 12.28%. The dissolution porosity of feldspar dissolution diagenetic facies increased the most, with an average of 3.95%. Clay mineral cemented microporous diagenetic facies lost the most porosity due to the middle and late cementation, with an average of 8.11%. The compaction of carbonate cemented tight diagenetic facies leads to the smallest loss of porosity, while the early cementation leads to the largest loss of porosity, which is 17.12%.


## 4. Differences in Microscopic Characteristics of Different Diagenetic Facies

### 4.1. Differences in Pore Throat Structure

Through the analysis of the size distribution of different types of pore throats and the control of physical properties in Figure4, it is found that the main peak value of mercury inflow and permeability contribution value of the residual chlorite-membrane intergranular-pore diagenetic facies are both at >1 μm. The main peak values of mercury inflow and permeability contribution from pore throats of the feldspar dissolution diagenetic facies are both between 0.5 μm and 1 μm. Due to the later cementation, the pore throat of the clay mineral cemented microporous diagenetic facies is seriously damaged, the pore throat configuration is poor, the number of mesopore throats is reduced, the pore throat mercury intake decreases, the cumulative mercury intake decreases, and the main peak of the pore throat radius of the contribution value of permeability and permeability is between 0.1 μm∼0.5 μm. The pore throats of the carbonate cemented tight diagenetic facies have almost disappeared. Unimodal is the main morphology that contributes to the pore throat radius interval and permeability. Permeability contribution rate and pore throat mercury ingress are the least. The main peak value of pore throat mercury ingress and permeability contribution value of pore throat radius are both at <0.1 μm.Figure 4
Different types of pressure curves and pore throat distribution characteristics. (a) Residual chlorite-membrane intergranular-pore diagenetic facies, A3, 1945.2 m. (b) Feldspar dissolution diagenetic facies, Y182, 2101.2 m. (c) Clay mineral cemented microporous diagenetic facies, A211, 1922.6 m. (d) Carbonate cemented tight diagenetic facies, Y144, 2178.4 m.
(a)(b)(c)(d)In the initial stage of mercury intrusion experiment, for samples with different permeability, the relatively large pore throat occupies a small proportion. However, the cumulative permeability contribution value rose rapidly to about 98% within the radius of the large pore throat. The cumulative mercury saturation in this interval is also increasing rapidly, and the curve is relatively steep, but the steepness is not as steep as the cumulative permeability contribution rate. The cumulative mercury saturation achieved in this interval is mainly distributed between 49% and 66%. Subsequently, mercury continued to enter the sample, and the cumulative permeability contribution curve showed a flat trend with a slow increase rate. However, the increase rate of accumulated mercury saturation did not decrease significantly. It shows that the relatively large pore throat mainly controls the permeability, and the relatively small pore throat has little effect on the permeability, but has a certain storage capacity. Through analysis of mercury intrusion samples in the study area, it was found that the average mercury saturation of about 29.5% was controlled by relatively small pore throats. The permeability of the study area is mostly controlled by pore throats with a radius larger thanR50∼R60.When the characteristics of mercury injection curves of different diagenetic facies are compared, it is found that the permeability contribution curve shifts to the left as the sample permeability decreases, indicating that the greater the permeability, the larger the proportion of relatively large pore throats, and vice versa. The diagenetic facies pore throat radius distribution is obviously different, which determines the permeability difference.


### 4.2. Differences in the Occurrence Characteristics of Movable Fluids

The movable fluid saturation of the residual chlorite-membrane intergranular-pore diagenetic facies samples of the chlorite membrane is the highest, which is 58.5%, of which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 44.8%, and the movable pore space corresponding to the T2 cut-off value is less than 13.7%. The morphological characteristics of the T2 spectrum curve before centrifugation showed a double-peak shape with high left and low right, and the T2 cut-off value was 4.97 ms. After centrifugation, the morphological characteristics of the T2 spectrum curve changed to a near-single peak shape (Figure 5(a)).Figure 5
NMRT2 spectrum distribution of different diagenetic facies. Note: the blue area is the movable pore space corresponding to the relaxation time greater than the T2 cut-off value, the pink area is the movable pore space corresponding to the relaxation time less than the T2 cut-off value, and the dashed line is the T2 cut-off value. (a) Residual chlorite-membrane intergranular-pore diagenetic facies, H393, 2247.3 m. (b) Feldspar dissolution diagenetic facies, H185, 226.5 m. (c) Clay mineral cemented microporous diagenetic facies, A296, 2197.6 m. (d) Carbonate cemented tight diagenetic facies, H26, 2199.9 m.
(a)(b)(c)(d)The movable fluid saturation of the feldspar dissolution diagenetic facies samples is medium, 35.66%, in which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 23.6%, and the movable pore space corresponding to the T2 cut-off value is 12%. The morphological characteristics of the T2 spectrum curve before centrifugation showed a double-peak shape of left high and right low type. After centrifugation, the right peak of the T2 spectrum curve decreased to a greater extent (Figure 5(b)).The movable fluid saturation of the clay mineral cemented microporous diagenetic facies sample is relatively small, 23.9%, of which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 18.2%, and the movable pore space corresponding to the T2 cut-off value is 5.7%. The T2 spectrum curve before centrifugation is characterized by a single peak shape, and the T2 spectrum curve shape after centrifugation mainly changes in the region greater than the T2 cut-off value (Figure 5(c)).The movable fluid saturation of the carbonate cemented tight diagenetic facies sample is the lowest at 12.69%, of which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 7.1%, and the movable pore space corresponding to the T2 cut-off value is 5.6%. The morphological characteristics of the T2 spectrum curve before centrifugation showed a single peak shape, and the shape of the T2 spectrum curve after centrifugation hardly changed significantly (Figure 5(d)).According to the above research and analysis, it is found that the movable fluid saturation and movable fluid porosity of the sandstone core samples of the low permeability reservoirs in the study area are generally low and have a large distribution range, and the microscopic pore structure heterogeneity is strong and the difference is large. TheT2 cut-off value is generally low. Most of the samples before and after centrifugation are smaller than the T2 cut-off value. The curve shape changes little. The area where the movable fluid saturation changes greatly is mainly the blue area, indicating the difference in the movable fluid saturation in the study area. It mainly depends on the degree of connectivity of the relatively large pore space corresponding to the relaxation time greater than the T2 cut-off value, and the movable fluid saturation varies significantly between different diagenetic facies.


## 4.1. Differences in Pore Throat Structure

Through the analysis of the size distribution of different types of pore throats and the control of physical properties in Figure4, it is found that the main peak value of mercury inflow and permeability contribution value of the residual chlorite-membrane intergranular-pore diagenetic facies are both at >1 μm. The main peak values of mercury inflow and permeability contribution from pore throats of the feldspar dissolution diagenetic facies are both between 0.5 μm and 1 μm. Due to the later cementation, the pore throat of the clay mineral cemented microporous diagenetic facies is seriously damaged, the pore throat configuration is poor, the number of mesopore throats is reduced, the pore throat mercury intake decreases, the cumulative mercury intake decreases, and the main peak of the pore throat radius of the contribution value of permeability and permeability is between 0.1 μm∼0.5 μm. The pore throats of the carbonate cemented tight diagenetic facies have almost disappeared. Unimodal is the main morphology that contributes to the pore throat radius interval and permeability. Permeability contribution rate and pore throat mercury ingress are the least. The main peak value of pore throat mercury ingress and permeability contribution value of pore throat radius are both at <0.1 μm.Figure 4
Different types of pressure curves and pore throat distribution characteristics. (a) Residual chlorite-membrane intergranular-pore diagenetic facies, A3, 1945.2 m. (b) Feldspar dissolution diagenetic facies, Y182, 2101.2 m. (c) Clay mineral cemented microporous diagenetic facies, A211, 1922.6 m. (d) Carbonate cemented tight diagenetic facies, Y144, 2178.4 m.
(a)(b)(c)(d)In the initial stage of mercury intrusion experiment, for samples with different permeability, the relatively large pore throat occupies a small proportion. However, the cumulative permeability contribution value rose rapidly to about 98% within the radius of the large pore throat. The cumulative mercury saturation in this interval is also increasing rapidly, and the curve is relatively steep, but the steepness is not as steep as the cumulative permeability contribution rate. The cumulative mercury saturation achieved in this interval is mainly distributed between 49% and 66%. Subsequently, mercury continued to enter the sample, and the cumulative permeability contribution curve showed a flat trend with a slow increase rate. However, the increase rate of accumulated mercury saturation did not decrease significantly. It shows that the relatively large pore throat mainly controls the permeability, and the relatively small pore throat has little effect on the permeability, but has a certain storage capacity. Through analysis of mercury intrusion samples in the study area, it was found that the average mercury saturation of about 29.5% was controlled by relatively small pore throats. The permeability of the study area is mostly controlled by pore throats with a radius larger thanR50∼R60.When the characteristics of mercury injection curves of different diagenetic facies are compared, it is found that the permeability contribution curve shifts to the left as the sample permeability decreases, indicating that the greater the permeability, the larger the proportion of relatively large pore throats, and vice versa. The diagenetic facies pore throat radius distribution is obviously different, which determines the permeability difference.


## 4.2. Differences in the Occurrence Characteristics of Movable Fluids

The movable fluid saturation of the residual chlorite-membrane intergranular-pore diagenetic facies samples of the chlorite membrane is the highest, which is 58.5%, of which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 44.8%, and the movable pore space corresponding to the T2 cut-off value is less than 13.7%. The morphological characteristics of the T2 spectrum curve before centrifugation showed a double-peak shape with high left and low right, and the T2 cut-off value was 4.97 ms. After centrifugation, the morphological characteristics of the T2 spectrum curve changed to a near-single peak shape (Figure 5(a)).Figure 5
NMRT2 spectrum distribution of different diagenetic facies. Note: the blue area is the movable pore space corresponding to the relaxation time greater than the T2 cut-off value, the pink area is the movable pore space corresponding to the relaxation time less than the T2 cut-off value, and the dashed line is the T2 cut-off value. (a) Residual chlorite-membrane intergranular-pore diagenetic facies, H393, 2247.3 m. (b) Feldspar dissolution diagenetic facies, H185, 226.5 m. (c) Clay mineral cemented microporous diagenetic facies, A296, 2197.6 m. (d) Carbonate cemented tight diagenetic facies, H26, 2199.9 m.
(a)(b)(c)(d)The movable fluid saturation of the feldspar dissolution diagenetic facies samples is medium, 35.66%, in which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 23.6%, and the movable pore space corresponding to the T2 cut-off value is 12%. The morphological characteristics of the T2 spectrum curve before centrifugation showed a double-peak shape of left high and right low type. After centrifugation, the right peak of the T2 spectrum curve decreased to a greater extent (Figure 5(b)).The movable fluid saturation of the clay mineral cemented microporous diagenetic facies sample is relatively small, 23.9%, of which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 18.2%, and the movable pore space corresponding to the T2 cut-off value is 5.7%. The T2 spectrum curve before centrifugation is characterized by a single peak shape, and the T2 spectrum curve shape after centrifugation mainly changes in the region greater than the T2 cut-off value (Figure 5(c)).The movable fluid saturation of the carbonate cemented tight diagenetic facies sample is the lowest at 12.69%, of which the movable pore space corresponding to the relaxation time greater than theT2 cut-off value is 7.1%, and the movable pore space corresponding to the T2 cut-off value is 5.6%. The morphological characteristics of the T2 spectrum curve before centrifugation showed a single peak shape, and the shape of the T2 spectrum curve after centrifugation hardly changed significantly (Figure 5(d)).According to the above research and analysis, it is found that the movable fluid saturation and movable fluid porosity of the sandstone core samples of the low permeability reservoirs in the study area are generally low and have a large distribution range, and the microscopic pore structure heterogeneity is strong and the difference is large. TheT2 cut-off value is generally low. Most of the samples before and after centrifugation are smaller than the T2 cut-off value. The curve shape changes little. The area where the movable fluid saturation changes greatly is mainly the blue area, indicating the difference in the movable fluid saturation in the study area. It mainly depends on the degree of connectivity of the relatively large pore space corresponding to the relaxation time greater than the T2 cut-off value, and the movable fluid saturation varies significantly between different diagenetic facies.


## 5. Conclusions

(1)
The early compaction of diagenesis in the study area resulted in an average porosity loss rate of 50.62%, the overall cementation caused a porosity loss rate of about 27.8%, and the dissolution increased the secondary porosity to an average of 2.26%. The porosity evolution characteristics of different diagenetic facies are obviously different, and the final calculated porosity of the residual chlorite-membrane intergranular-pore diagenetic facies is the largest, with an average of 12.28%. The dissolution porosity of the feldspar dissolution diagenetic facies increases the most, with an average of 3.95%. The clay mineral cemented microporous diagenetic facies lose the most porosity due to the middle-late cementation, with an average of 8.11%. The carbonate cemented tight diagenetic facies lead to the smallest loss of porosity, while the early cementation leads to the largest loss of porosity, with an average of 17.12%.(2)
There are obvious differences in pore throat radius distribution characteristics, movable fluid occurrence characteristics, and water drive characteristics of different diagenetic facies. The size distribution of the pore throat radius controls the seepage capacity. The larger the proportion of relatively large pore throats, the greater the permeability and the stronger the seepage capacity. The pore throat distribution with a radius greater thanR50∼R60 determines the permeability. The difference of movable fluid saturation mainly depends on the degree of connectivity of the relatively large pore space corresponding to the relaxation time greater than the T2 cut-off value.



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*Source: 5611786-2021-09-02.xml*