# Diagenetic Fluid and Its Impact on Sandstone Reservoirs in the Southern Boxing Sag, Dongying Depression, Bohai Bay Basin, China

Authors: Zhenhuan Shen; Zhuang Ruan; Bingsong Yu; Shujun Han; Chenyang Bai; Qiuhong Chang; Tianxia An
Journal: Geofluids
 (2022)

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## Abstract

Diagenesis typically exerts a crucial impact on the formation of high-quality sandstone reservoirs in the Eocene Shahejie Formation, Dongying Depression. To better understand the formation process of petrophysical properties, this research conducts petrographic and geochemical analyses to investigate the nature of diagenetic fluids. Petrographic observations suggest that the dominant cements are carbonate, authigenic quartz, and clay minerals, accompanied with the dissolution of feldspar and calcite. The homogenization temperature of aqueous inclusions in quartz overgrowth usually exceeds 90°C corresponding to the maturity of organic matter. Quartz overgrowths contain higher amounts of CaO and Al2O3 than detrital quartz. This indicates that the siliceous fluid mainly originates from the dissolution of feldspar. Moreover, the conversion of clay minerals also provides trace amounts of silica into pore water during the burial process. Carbonate cements consist of early-stage calcite as well as late-stage Fe-calcite and ankerite. Calcite with relatively higher MnO proportions shows yellow luminescence and dissolution signs. Fe-calcite and ankerite cements have a higher homogenization temperature than that of quartz overgrowth and mainly concentrate in FeO and MgO as well as contain a small amount of Na+, K+, and Sr2+. The rare earth element (REE) pattern of bulk mudstone and carbonate cements as well as C–O isotopic evidences indicate that the diagenetic fluids of carbonate cementation are primarily controlled by the adjacent mudstone, whereas mineral dissolution and altered clay minerals in sandstone provide additional cations for the local reprecipitation of late-stage carbonate. Therefore, diagenetic fluids within sandstone reservoirs are typically subject to alkaline–acid–alkaline conditions and are influenced by internal sources in a closed system. Compaction significantly reduces the pore space of sandstone reservoirs in the Boxing Sag. Carbonate cementation further increases the complexity of pore structure and obeys the principle of mass balance.


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## Body

## 1. Introduction

Diagenesis including compaction, cementation, metasomatism, and dissolution crucially determines the development of pore space within siliciclastic rock reservoirs (e.g., [1–4]). In particular, cementation and dissolution are closely related to the geochemical properties of pore fluids and record the signal of water–rock reactions during progressive diagenesis [5, 6]. Nevertheless, the characteristics of pore fluids are typically complicated and vary in different diagenetic stages [7, 8]. Thus, it is significant to comprehend the diagenetic stages and fluid properties in burial environment for revealing the evolution of diagenetic fluids and the formation of high-quality reservoirs [9]. Currently, several reliable methods for dividing diagenetic stages exist, including clay mineral composition, vitrinite reflectance, and organic matter maturity [3, 10, 11]. However, the origin of fluids, temperature conditions for fluid activity, and transformation time of diagenetic fluids are still debatable [12, 13]. The use of major and minor elements together with C–O isotope of carbonate minerals was the most widespread methods to track the source of fluids and the organic–inorganic reactions in siliciclastic rock reservoirs (e.g., [14–19]). Fluid inclusions within authigenic minerals were conducted to ascertain the time of fluid combining with the burial history [20–22] and provided additional evidence to distinguish the origin of diagenetic fluids [23]. Over the past few years, electron probe microanalysis (EPMA), laser ablation inductively coupled plasma-mass spectrometry (LA-ICP-MS), and secondary ion mass spectrometry (SIMS) were gradually applied in diagenetic fluid research owing to the development of in situ testing technologies (e.g., [24–26]), which helped in revealing fluid characteristics and in understanding diagenetic transformation during the burial process.The Eocene Shahejie Formation in the Boxing Sag, southern Dongying Depression, is a significant oil-bearing reservoir, which primarily comprises interbedded very fine-grained sandstones, siltstones, and mudstones in an open littoral and shallow lacustrine sedimentary environment [27–29]. Sandstones in the Shahejie Formation normally underwent complicated diagenesis. Previous studies have demonstrated that compaction is the primary factor for reducing the reservoir properties, followed by cementation, further increasing the heterogeneities of the pore structure as well as decreasing the reservoir porosity and permeability [21, 22, 30]. Carbonate minerals, authigenic quartz, and clay minerals are the most common diagenetic cements within sandstones in the Boxing Sag. The distance from sandstone to mudstone has a crucial influence on carbonate precipitation because compacted mudstones release sufficient ions into pore water [30, 31]. The silica source for quartz overgrowth normally stems from feldspar dissolution and is mainly determined by the petrographic evidences [6, 29]. However, few comprehensive studies have focused on the characteristics and sources of fluids for carbonate and quartz cements to explain diagenetic transformation within reservoirs in the Boxing Sag. Additionally, mineral dissolution induced by the thermal evolution of organic matter in an open or closed diagenetic system probably determines whether the by-products mass transfer and reservoir quality can be improved [32, 33]. Therefore, the research of diagenetic fluid provides valuable information about the cementation origin and helps in further exploring the water–rock reactions and fluid migration within reservoirs.This study is primarily aimed at revealing the characteristics and origins of diagenetic fluids and their influence on sandstone reservoirs. We focused on (1) building the diagenetic sequences of sandstone reservoirs using petrographic features, (2) utilizing quantitative methods, including the homogenization temperature of fluid inclusions, major and trace elements, and stable isotopic analysis to investigate the sources and transformation time of diagenetic fluids, and (3) discussing the geochemical diagenesis system and its impact on the quality of reservoirs in the Eocene Shahejie Formation beach-bar sandstones.


## 2. Geological Setting

The Bohai Bay Basin, located in eastern China, is an important hydrocarbon-producing basin. It comprises several subbasins and covers approximately 200,000 km2 (Figure 1(a)). The Jiyang Subbasin is bounded by the Tanlu Fault to the east, Chengning Uplift to the northwest, and Luxi Uplift to the south. The Dongying Depression is a secondary tectonic unit of the Jiyang Subbasin and has an area of approximately 5700 km2 (Figure 1(b)). It is situated in the southeastern part of the Jiyang Subbasin and is bordered by the Luxi Uplift to the south, Guangrao rise to the southeast, Chengjiazhuang rise to the north, and Binxian and Qingcheng rises to the west. The Dongying Depression comprises the southwestern Boxing, central Niuzhuang, northwestern Lijing, northeastern Minfeng sags, and central diapiric anticline (Figure 1(c)).Figure 1
(a, b) Structural map of the Bohai Bay Basin and tectonic setting of the Dongying Depression. (c) Cross-section of B–B’ in the Boxing Sag (modified from [64]).The Boxing Sag, the study area, contains Cenozoic sediments hosting six formations, upward namely the Paleogene Kongdian (Ek), Shahejie (Es) and Dongying (Ed), Neogene Guantao (Ng) and Minghuazhen (Nm), and Quaternary Pingyuan (Qp) formations. The Es Formation is divided into four members: Es1, Es2, Es3, and Es4, from the top to the bottom in the specified order. The Es4 and Es3 members can be further divided into several submembers based on the differences in petrological properties. These submembers are called Es4x, Es4s, Es3x, Es3z, and Es3s from the bottom to the top. The Es4s and Es3x, which are dominated by thin-bedded very fine-grained sandstones and siltstones interbedded with mudstone, are the research objects of this study (Figure2). During the Es4s sedimentary period, the different sags in the Dongying Depression were connected. Furthermore, the sand bodies of a deltaic deposit were developed on the southern gentle slope with an abundant supply of fluvial sediments. Owing to the development of certain humps on the gentle slope and the subsequent wave action, characteristic beach-bar sandstones deposited in the broad-shore shallow-lake environment and frequently interbedded with mudstone and shale [27]. This depression entered a relatively deep-lacustrine environment during the Es3 sedimentary period because the basement quickly subsided [34]. Sand bodies of deltaic deposits can be found at the south and west margins of the Boxing Sag. Meanwhile, it is characterized by beach-bar sandstones mixed with micrite and oolitic limestones in thick mudstones in the central part of the study area.Figure 2
Tertiary stratigraphy and tectonic evolution of the Dongying Depression; sedimentary sequence of wells F104 and G351 in the Es3x and Es4s, respectively, and their locations are shown in Figure1(b).


## 3. Materials and Methods

A total of 30 samples from 7 wells (F25, G351, and F104 in the Es3x interval; F1, G893, G891, and G351 in the Es4s interval) in the Boxing Sag were prepared into blue epoxy resin-immersed thin sections (30μm thickness) (Figure 1(b)), which were partly stained with Alizarin red-S and K-ferricyanide for petrographic and carbonate minerals observation under the Olympus BX51 microscope. 20 thin sections were selected for cathodoluminescence (CL) observation conducted by the LeicaDM2500P microscope with a voltage of 12 kV and current of 250 μA. Four thin sections were coated by a Pt-conducting layer and then observed under a Zeiss Supra 55 field emission scanning electron microscope (SEM) with 20 kV accelerating voltage. Secondary electron imaging and AsB detector were applied to characterize morphological features and reveal compositional difference, respectively. The SEM was equipped with energy-dispersive X-ray spectrometer (EDS) to analyse the elemental concentrations at a spot. Four doubly polished sections approximately 100 μm thick were prepared for fluid inclusion measurement on quartz overgrowth and carbonate cements by a Linkam TH600 heating-freezing stage. Homogenization temperatures (Th (°C)) were measured for fluid inclusions using a heating rate of 25°C/min at temperatures less than 70°C and a rate of 5 or 3°C/min at temperatures exceeding 70°C. The above-mentioned experiments were carried out at the State Key Laboratory of Geological Processes and Mineral Resources of China University of Geoscience (Beijing).Porosity and permeability data of 588 core plugs (2.5 cm diameter) and X-ray diffraction (XRD) data of 75 samples from the Shahejie sandstone reservoirs were collected from Shengli Oilfield Company, Sinopec. The porosity and permeability were analyzed using the CMStm-300 Core Measurement with N2 and a confining pressure of 6 MPa. The XRD analysis of the powdered samples (less than 40 mm) was conducted by using a D/max-2500 theta/theta rotating anode X-ray diffractometer.Four sandstone samples from wells F1, F25, G351, and F104 were cut into cubes of around 1 cm3 for high-pressure mercury injection (HPMI) experiment at the Key Laboratory of Tectonics and Petroleum Resources of China University of Geosciences (Wuhan). These cubes were first oven dried at 60°C for over 48 hours to remove volatile substances and moisture and then cooled to room temperature (about 23°C) in a desiccator. The experiment was conducted with the Autopore IV 9520 mercury injection instrument with a maximum pressure of 414 MPa.The C-O isotopes, electron probe microanalysis (EPMA), and rare earth element (REE) of mudstone experiments were conducted on the Analytical Laboratory of the Research Institute of Uranium Geology (Beijing). Based on petrology observation, 13 carbonate-cemented sandstone samples were selected for carbon and oxygen isotope tests. Samples were drilled by a microdrill bit with a diameter of 2 mm for powder less than 200 meshes. Carbon and oxygen isotopes were measured by adding concentrated phosphoric acids to produce the CO2 which were tested by a MAT-253 gas isotope mass spectrometer. Isotopic compositions are reported in the standard delta notation as per mill (‰) relative to Vienna Pee Dee Belemnite (VPDB), with an analytical precision of ±0.2‰ for carbon isotopes and ±0.1‰ for oxygen isotopes.EPMA was conducted for six samples by a JXA-8100 instrument at 20 kV accelerating voltage,1×10−8A beam current, and 3 to 5 μm beam diameter. The major elements measured in the quartz overgrowth and carbonate include Al, Na, Mg, K, Ca, Sr, Ni, Ti, Fe, Cr, and Mn.The microdrilling samples of mudstones were analyzed for REE. About 25 mg powder was dissolved by 1 mL HF and 0.5 mL HNO3 in a closed container, which was heated for 24 hours at about 185°C in an oven. Then, the container was steamed to dry in an electric heating plate and added 0.5 mL HNO3 to evaporate. This step was repeated once. After that, 5 mL HNO3 was put into container and heated for 3 hours at 130°C. Finally, the solution was transferred into a plastic bottle and diluted to 25 mL as well as measured through an Element XR inductively coupled plasma-mass spectrometry (ICP-MS).The REE of carbonate cement experiments were carried out on Analytik Jena AG PlasmaQuant MS Plus, ICP-MS instrument, in combination with an excimer 193 nm laser ablation system (NWR193 UItra Compact). Each spot analysis consisted of approximately 30s background acquisition followed by 40s data acquisition form the sample. Calibration was performed using NIST SRM610 and 614as external calibrant in conjunction with internal standardization using CaO. Data reduction was made using the GLITTER 4.0 software.


## 4. Results

### 4.1. Detrital Petrology

Petrographic investigation shows that the grain sizes of beach-bar sandstones mainly range between 0.021 and 0.421 mm, of which the average 49.9% of the grains are 0.063–0.125 mm (very fine sand), 34.0% of the grains are 0.125–0.25 mm (fine sand), 7.5% of the grains are 0.25–0.50 mm (medium sand), and 7.4% of the grains are 0.031–0.063 mm (coarse silt). Sorting ranges from medium to good sorted and roundness of the detrital particles are hypoedge angle for most of the sandstones (Table1).Table 1
Thin-section compositions from optical point counting and quantitative image analysis.
WellStrataNo.Grain size (mm), %SoNo.Quartz, %K-feldspar, %Plagioclase, %Rock fragment, %0.031–0.0630.063–0.1250.125–0.250.25–0.50F1Es4314.260.924.901.6640.714.418.226.7F25Es32010.152.237.71.5243.516.020.020.5F104Es320.535.8558.74.951.61739.415.719.325.7G351Es426.760.9531.151.21.51648.316.517.517.7G891Es4112.163.324.30.31.6246.417.919.815.9G893Es4218.868.312.901.5745.917.719.615.87.549.934.07.4AVG.44.116.419.120.4Sorting coefficientSo=P25/P75, P25, and P75 are the grain sizes at 25% and 75%, respectively.The detrital compositions of beach-bar sandstones comprise 39.4%–48.3% quartz (average 44.1%), 14.4%–17.9% K-feldspars (average 16.4%), 17.5–20.0% plagioclase (average 19.1%), and rock fragments 15.8%–26.7% (average 20.36%) (Table1). The rock fragments are mainly composed of volcanic rocks, metamorphic rocks, and a little sedimentary origin. The composition of sandstones is immature with an average framework composition of Q44.1F35.5L20.4. Thus, beach-bar sandstones are mostly lithic arkoses based on the Folk [35] classification standard (Figure 3).Figure 3
Rock composition of the beach-bar sandstones in the Boxing Sag. Based on the classification standard of Folk et al. [35].


### 4.2. Diagenetic Mineralogy

#### 4.2.1. Feldspar Diagenesis

Feldspars, including K-feldspars and plagioclases, were partly to fully dissolved in the beach-bar sandstones, which was associated with the precipitation of authigenic quartz and clay minerals (Figures4(a) and 4(b)). The internal fabric of the partly dissolved feldspar could still be applied to distinguish among the composition of inherited minerals (Figures 4(b)–4(d)). On the whole, the secondary intragranular pores resulting from the dissolution of detrital feldspars as well as the primary intergranular pores were filled with newly formed minerals. Microscopy and SEM analysis showed that authigenic quartz mainly existed as quartz overgrowths and microquartz (Figures 4(e), 4(f), and 5(a)). The former was usually observed on the margin of quartz grains whose thickness could reach approximately 30 μm. Actually, quartz cements with exceptionally fine grains were difficult to identify in the sandstone (Figure 4(e)). A large number of microquartz crystals of only a few microns in size filled the gaps between the grains. Moreover, authigenic feldspar (albite) was also generated as overgrowths and well-crystallized grains under the SEM (Figure 5(b)), but it was not as common as authigenic quartz.Figure 4
Photomicrographs of carbonate cements, dissolved feldspars and secondary minerals in thin sections. (a) F1, 3321.5 m: the dissolution of calcite and feldspar with the precipitation of secondary quartz; (b) F25, 2998.5 m: the leached feldspar and associated secondary minerals; (c) G351, 2444.5 m: feldspar dissolution and Fe-calcite and ankerite precipitation; (d) G351, 2447 m: the leached feldspar and associated secondary minerals, and the secondary intragranular pore is destroyed by ankerite precipitation; (e) F1, 3314.6 m: the precipitation of secondary quartz mineral with a width of approximate 40μm; (f) F104, 3038.9 m: the leached feldspar and associated quartz overgrowths; (g) G891, 2808.4 m: early calcite cement and late ankerite cement; (h) G351, 2444.5 m: the dissolution of calcite and feldspar accompanied by clay minerals, and ankerite cement; (i) F1, 3319.1 m: the intergranular pores are destroyed by ankerite cements. Note: Qo: quartz overgrowth, R: rock fragment, Fd: feldspar dissolution, Cc: calcite, Fc: ferrocalcite, and An: ankerite.
(a)(b)(c)(d)(e)(f)(g)(h)(i)Figure 5
SEM-BSE images of beach-bar sandstones in the Boxing Sag. (a) F1, 3314.6 m: authigenic microquartz (Mq) and a few clay minerals; (b) F1, 3314.6 m: authigenic albite (Ab); (c) G351, 2455 m: the feldspar dissolution is accompanied by the precipitation of illite (yellow arrow); (d) G351, 2455 m: barite (yellow arrow) and pyrite (Py) are filled among particles; (e) F1, 3314.6 m: the leached detrital grain associated with chlorite (yellow arrow), and red spot represents an EDS analyzing point; (f) EDS-tested composition of the barite (BaSO4).
(a)(b)(c)(d)(e)(f)


#### 4.2.2. Carbonate Diagenesis

Three types of carbonate cements dominated by calcite, Fe-calcite, and ankerite could be distinguished in the sandstone reservoirs. Different types of carbonate cements could be formed in different periods during the diagenesis process and indicate the pore water characteristics. Calcites occupied the primary pore spaces among clastic grains, displayed the dissolved feature, and showed yellow luminescence (Figures4(g), 4(f), 6(a), and 6(b)). Generally, sandstones containing calcite cements were normally supported by clastic grains with point contacts or exhibited floating structures (Figure 4(h)). Fe-calcites with dark red luminescence filled the intergranular pores and secondary intragranular pores of the dissolved feldspars (Figures 4(c), 6(c), and 6(d)). Ankerites with dark luminescence occupied the intergranular pores and exhibited euhedral rhombs growing in the dissolved feldspar pores and replacing the preexisting calcite (Figures 4(d), 4(h), and 4(i)).Figure 6
Cathodoluminescence (CL) observation of carbonate cements. (a, b) F1, 3319.1 m: calcite (Cc) and ankerite show the yellow and dark luminescence, respectively; (c, d) F104, 3059.4 m: the dissolution of feldspar (F) and Fe-calcite show the dark red luminescence.
(a)(b)(c)(d)


#### 4.2.3. Clay and Other Minerals

The observation conducted on thin sections showed that feldspar dissolution was accompanied with clay mineral precipitation. SEM analysis revealed the presence of clay minerals with fibrous and flaky features in feldspar dissolution pores and grew together with minor amounts of microcrystalline authigenic quartz (Figures5(a) and 5(c)). Needle-shaped chlorite could be observed in the dissolved pores (Figure 5(e)). X-ray diffraction data of bulk rocks showed that the mixed-layer illite/smectite and kaolinite, followed by illite and chlorite, are the clay minerals found in majority in the Boxing sandstone reservoirs (Figure 7). The content of mixed-layer illite/smectite decreased at 1750 to 2600 m and then increased from 2600 to 3250 m. However, the mixed-layer ratio (S% in I/S) apparently decreased as the depth increased. The content of kaolinite increased at 1750 to 2600 m and decreased at 2600 to 3250 m as the depth increased. The content of chlorite did not exceed 25% and hardly varied in the vertical distribution.Figure 7
Vertical distribution characteristics of clay minerals in the Boxing Sag.Besides, barite (BaSO4) exhibiting an irregular shape filled among the clastic grain gaps and could be identified via the SEM-EDS analysis in the wells F1 and G351 (Figures 5(d)–5(f)). Pyrite comprised of nodule-shaped aggregates and occurred as a variant of pore-filling cement (Figure 5(d)).


### 4.3. Petrophysical Characteristics

The Shahejie Formation sandstone samples in the Boxing Sag exhibited widely distributed porosity and permeability ranging from 1.2% to 32.7% and from 0.023 to 1276 mD as well as from 2.6% to 28.0% and from 0.007 to 152.28 mD, respectively. Generally, the sample porosity and permeability decreased as the burial depth increased from 1500 to 3500 m (Figures8(a) and 8(b)). Based on the reservoir classification from Zeng and Li [36], 34.8% and 48.7% of the Es3 and Es4 sandstones, respectively, were low-porosity reservoirs; their porosity was less than 15.0% (Figure 8(c)); 87.2% and 82.7% of the Es3 and Es4 sandstones, respectively, were low-permeability reservoirs; their permeability was less than 50.0 mD (Figure 8(d)).Figure 8
Petrophysical properties of sandstones in the Es3 and Es4 Formation in the Boxing Sag. (a, b) Vertical distribution of porosity and permeability. (c, d) Histogram distribution of porosity and permeability; the red dash lines distinguish low-porosity and low-permeability reservoirs.The high-pressure mercury intrusion (HPMI) analysis of four beach-bar sandstone samples also satisfied the characteristics of low-porosity and low-permeability sandstone reservoirs. In particular, the permeability was usually less than 1 mD. The distribution of pore throat radius mainly ranged between 0.01 and 1μm depending on the micropore size (Figure 9).Figure 9
Typical pore throat radius distribution obtained from the HPMI experiment.


### 4.4. Fluid Inclusions

Fluid inclusions in authigenic minerals (quartz overgrowth and carbonate) could provide information about the diagenetic environment. Nevertheless, quartz overgrowths could not be easily identified as the grain sizes were dominated by very fine sand in certain wells, and the size of two-phase fluid inclusions in the quartz overgrowths was mainly less than 6μm (Figures 10(a)–10(c)). Together, these factors posed great challenges to the measurement of the homogenization temperature. Herein, the adjacent wells and samples of similar depth were selected for measuring the Th (°C) of aqueous inclusions (Table 2). The Th (°C) of quartz overgrowths mainly ranged between 99°C and 129°C in the Es3x Formation (Figure 11(a)). The Th (°C) from well G351 ranged between 106°C and 121°C in the Es4s Formation (Figure 11(b)). Meanwhile, the fluid inclusions within carbonate cements of wells F104 and F25 were extremely small and rarely found. The Th (°C) mainly ranged between 118°C and 126°C in the Es3 Formation (Figures 10(d) and 11(a)).Figure 10
Petrography of fluid inclusions within quartz overgrowths (Qo) and carbonate cementation (Cc) in sandstones.
(a)(b)(c)(d)Table 2
Microthermometric data of fluid inclusions in the authigenic minerals.
WellDepth (m)StrataHost mineralTh (°C)WellDepth (m)StrataHost mineralTh (°C)F252998.5Es3Qo113F1823109.5Es3Qo115.7F252998.5Es3Qo129F1823109.5Es3Qo116.8F252998.5Es3Qo117F1823109.5Es3Qo111.1F252998.5Es3Qo116G3512444.45Es4Qo106F252998.5Es3Qo116G3512444.45Es4Qo105F1043038.9Es3Qo110G3512444.45Es4Qo115F1043038.9Es3Qo115G3512444.45Es4Qo121F1043038.9Es3Qo120G3512444.45Es4Qo108F1043038.9Es3Qo109G3512444.45Es4Qo113F1043038.9Es3Qo99F252998.5Es3Cc118F1043038.9Es3Qo102F252998.5Es3Cc121F1043038.9Es3Qo111F252998.5Es3Cc119F1823109.5Es3Qo124.1F252998.5Es3Cc119F1823109.5Es3Qo108.3F252998.5Es3Cc121F1823109.5Es3Qo120.7F1043038.9Es3Cc123F1823109.5Es3Qo117.9F1043038.9Es3Cc126F1823109.5Es3Qo106.8Qo: quartz overgrowth; Cc: carbonate cementation.Figure 11
Histogram of Th for fluid inclusions in the quartz overgrowths and carbonate cements. (a) Es3 Formation; (b) Es4 Formation.
(a)(b)


### 4.5. Geochemical Characteristics

The carbon and oxygen isotopic compositions of carbonate cements in the Es4 Formation sandstones show that theδ18O values range between −11.7‰ and −8.4‰, and the δ13C values range between −1.7‰ and −0.5‰. The isotopic δ18O and δ13C values of carbonate cements in the Es3x Formation sandstone range between −12.8‰ and −9.5‰ and between 1.6‰ and 3.3‰, respectively (Table 3).Table 3
Mineralogical and isotopic composition of carbonate. Ca: calcite; Fc: Fe-calcite; An: ankerite.
WellLithologyDepthStrataCarbonate contentMineralsδ18O−PDB (‰)δ13C−PDB (‰)F1Sandstone3321.5Es414.2%70%An+30%Ca-11.3-0.8F1Sandstone3319.1Es413.6%100%An-9.6-0.5F1Sandstone3314.6Es47.4%80%An+20%Ca-11.7-1.1F1Sandstone3312.3Es48.9%80%An+20%Ca-11.4-1.2F1Sandstone3310.3Es43.4%100%An-10-0.8F1Sandstone3311.3Es43.7%100%An-10.3-1G893Sandstone3210.2Es4—95%An+5%Ca-8.4-0.3G893Sandstone3281.0Es425.1%90%An+10%Ca-9.3-1.7F31Sandstone2934.0Es34.6%100%An-12.13F25Sandstone2901.5Es310.2%90%Fc+10%Ca-12.83.3F25Sandstone2998.5Es32.8%90%Fc+10%Ca-13.81.6F104Sandstone3038.9Es316.2%95%An+5%Fc-13.43.3F104Sandstone3039.2Es314.1%95%An+5%Fc-9.52.9The EPMA analysis was conducted to investigate the chemical differences between detrital and authigenic quartz as well as carbonate cements. The results obtained from this analysis of quartz particles showed that CaO and Al2O3 were slightly enriched in authigenic quartz content compared with the detrital phase. Moreover, the chemical compositions of quartz overgrowths at the inner and outer points exhibited no obvious differences (Table 4). The calcite normally displayed a high content in MnO. Fe-calcite and ankerite always had higher content of FeO and/or MgO and a slightly higher content of SrO, Na2O, Al2O3, and K2O than calcite (Table 5).Table 4
Electronic probe microanalysis for quartz in the Es3 sandstone (wt%).
WellDepth (m)PointMgONa2OFeOCaOAl2O3MnOK2OSrOTiO2SiO2TotalF312934.0Q000.030.0200.0200.33099.399.7Qo00.030.020.030.14000.330.0298.699.17Qo0000.050.17000.27098.498.89Q000.0200.0700.030.340.0299.2699.74Qo0000.050.1400.020.290.0299.2399.75Qo0000.020.0500.010.290.0499.0399.44F252998.5Q0.030.02000000.270.0499.4699.82Qo0.0200.040.110.19000.36098.5899.3Qo0.05000.250.200.020.37098.3899.27F1043039.2Q0.020.0400.040.04000.36099.53100.03Qo00.0200.030.18000.29098.999.42Qo0000.080.090.0300.35098.6499.19Q00.03000.02000.29099.1999.53Qo0000.020.17000.35098.899.34Qo00.040.020.050.1200.020.3099.1699.71Table 5
Electronic probe microanalysis for carbonate cements in the sandstone (wt%).
WellDepth (m)MgONa2OFeOCaOAl2O3MnOK2OSrOTiO2Cr2O3CO2TotalF13314.60.270.000.1653.890.031.440.000.040.000.0043.6799.500.250.000.1453.580.031.650.000.000.030.0043.5299.208.990.0015.0630.890.040.540.020.100.000.0043.7399.378.440.0316.6930.240.020.400.000.000.030.0043.4999.34F13311.30.390.001.7053.610.020.360.150.110.000.0043.91100.250.290.020.0554.500.060.700.000.000.000.0043.6799.298.620.1316.3130.770.000.270.040.030.000.0043.87100.048.980.0014.2931.780.040.420.060.270.000.0244.0099.86F3129349.030.0313.5632.690.000.350.030.250.000.0044.20100.149.540.0313.2132.020.000.370.000.110.030.0043.9999.30F252998.50.210.030.5354.790.000.030.030.000.000.0243.6699.300.160.000.5154.700.030.030.020.000.000.0243.5098.970.340.102.2152.840.040.220.000.000.000.0043.7499.490.260.091.7553.170.030.280.010.000.020.0043.5899.18F252901.50.540.001.9253.550.180.170.000.000.000.0044.25100.610.540.042.5652.810.020.200.020.000.000.0043.83100.01F1043038.99.020.0015.5030.840.170.200.070.220.000.0244.12100.160.470.181.3252.700.070.140.070.790.000.0043.3699.100.370.191.2553.550.050.140.030.770.000.0043.85100.200.350.001.2453.300.050.120.000.760.000.0043.4499.260.680.101.2152.510.080.110.090.860.000.0043.3598.990.690.041.1353.300.080.120.060.740.000.0043.86100.029.150.0012.7132.970.000.340.000.280.000.0044.0299.47F1043039.20.390.001.6253.490.020.240.000.100.000.0043.6299.480.310.041.4253.840.000.170.130.220.000.0043.7699.89The REE data of carbonate cements and mudstones are shown in Table6, displaying a high content of light REE (LREE) and a low content of heavy REE (HREE). The REE concentrations have been normalized by chondrite from Boynton [37] and given the subscript N. The δCe and δEu values are calculated by 2CeN/LaN+PrN and 2EuN/SmN+GdN, respectively. The δCe value of carbonate cement and mudstone ranged from 0.38 to 1.08 and from 0.87 to 0.94, with average values of 0.81 and 0.90, respectively. The δEu value of carbonate cement ranged between 0.14 and 2.63, with an average value of 1.10. It had a relatively wider distribution than that of mudstone whose δEu value ranged between 0.51 and 0.61.Table 6
The REE data of carbonate cement and mudstone (μg/g).
REEF25: 2901.5 m (n=3)F25: 2998.5 m (n=4)F104: 3039.2 m (n=4)F104: 3059.4 m (n=3)F1: mudstone (n=4)La20.193.1036.072.832.206.376.818.140.766.995.286.029.1928.1149.3052.3048.1055.60Ce34.745.0360.586.431.7317.2719.5513.300.957.306.1213.194.9239.1290.2099.1084.0094.90Pr4.430.784.930.800.212.452.771.450.060.730.512.000.333.6010.8011.409.2211.10Nd17.783.4513.684.391.0510.4113.495.310.202.502.209.901.9311.7940.8045.8033.4042.80Sm3.790.674.501.140.432.904.120.590.050.170.442.970.471.386.937.554.666.30Eu1.410.121.120.380.260.541.190.430.000.240.100.910.180.391.341.390.851.00Gd4.721.054.111.010.411.733.750.980.040.420.332.100.271.016.206.234.585.32Tb0.480.030.410.270.040.351.000.140.010.050.080.500.060.191.011.040.820.89Dy2.550.152.591.530.502.075.750.680.050.350.523.300.401.035.475.504.554.92Ho0.520.120.600.310.080.441.010.140.010.110.090.740.120.251.001.030.970.89Er1.670.281.720.780.221.202.770.540.050.180.342.200.050.672.943.063.042.60Tm0.32<0.00.150.150.040.160.330.060.000.020.070.33<0.00.030.470.470.480.41Yb1.040.060.710.660.230.961.930.340.050.160.292.050.320.563.143.333.343.16Lu0.080.030.170.080.030.140.260.050.010.030.040.300.040.110.430.450.490.40ΣREE93.7314.86131.3320.757.4246.9764.7332.172.2419.2516.4046.5218.2688.23220.02238.66198.49230.28LREE82.3413.15120.8815.975.8739.9347.9329.222.0117.9314.6535.0017.0184.38199.37217.54180.23211.70HREE11.391.7210.454.781.547.0416.802.950.221.321.7511.521.253.8520.6521.1218.2618.58δCe0.850.760.961.020.481.051.080.860.810.630.710.910.380.810.900.940.900.87δEu1.020.430.781.061.880.680.911.710.142.630.781.071.390.960.610.600.550.51


## 4.1. Detrital Petrology

Petrographic investigation shows that the grain sizes of beach-bar sandstones mainly range between 0.021 and 0.421 mm, of which the average 49.9% of the grains are 0.063–0.125 mm (very fine sand), 34.0% of the grains are 0.125–0.25 mm (fine sand), 7.5% of the grains are 0.25–0.50 mm (medium sand), and 7.4% of the grains are 0.031–0.063 mm (coarse silt). Sorting ranges from medium to good sorted and roundness of the detrital particles are hypoedge angle for most of the sandstones (Table1).Table 1
Thin-section compositions from optical point counting and quantitative image analysis.
WellStrataNo.Grain size (mm), %SoNo.Quartz, %K-feldspar, %Plagioclase, %Rock fragment, %0.031–0.0630.063–0.1250.125–0.250.25–0.50F1Es4314.260.924.901.6640.714.418.226.7F25Es32010.152.237.71.5243.516.020.020.5F104Es320.535.8558.74.951.61739.415.719.325.7G351Es426.760.9531.151.21.51648.316.517.517.7G891Es4112.163.324.30.31.6246.417.919.815.9G893Es4218.868.312.901.5745.917.719.615.87.549.934.07.4AVG.44.116.419.120.4Sorting coefficientSo=P25/P75, P25, and P75 are the grain sizes at 25% and 75%, respectively.The detrital compositions of beach-bar sandstones comprise 39.4%–48.3% quartz (average 44.1%), 14.4%–17.9% K-feldspars (average 16.4%), 17.5–20.0% plagioclase (average 19.1%), and rock fragments 15.8%–26.7% (average 20.36%) (Table1). The rock fragments are mainly composed of volcanic rocks, metamorphic rocks, and a little sedimentary origin. The composition of sandstones is immature with an average framework composition of Q44.1F35.5L20.4. Thus, beach-bar sandstones are mostly lithic arkoses based on the Folk [35] classification standard (Figure 3).Figure 3
Rock composition of the beach-bar sandstones in the Boxing Sag. Based on the classification standard of Folk et al. [35].


## 4.2. Diagenetic Mineralogy

### 4.2.1. Feldspar Diagenesis

Feldspars, including K-feldspars and plagioclases, were partly to fully dissolved in the beach-bar sandstones, which was associated with the precipitation of authigenic quartz and clay minerals (Figures4(a) and 4(b)). The internal fabric of the partly dissolved feldspar could still be applied to distinguish among the composition of inherited minerals (Figures 4(b)–4(d)). On the whole, the secondary intragranular pores resulting from the dissolution of detrital feldspars as well as the primary intergranular pores were filled with newly formed minerals. Microscopy and SEM analysis showed that authigenic quartz mainly existed as quartz overgrowths and microquartz (Figures 4(e), 4(f), and 5(a)). The former was usually observed on the margin of quartz grains whose thickness could reach approximately 30 μm. Actually, quartz cements with exceptionally fine grains were difficult to identify in the sandstone (Figure 4(e)). A large number of microquartz crystals of only a few microns in size filled the gaps between the grains. Moreover, authigenic feldspar (albite) was also generated as overgrowths and well-crystallized grains under the SEM (Figure 5(b)), but it was not as common as authigenic quartz.Figure 4
Photomicrographs of carbonate cements, dissolved feldspars and secondary minerals in thin sections. (a) F1, 3321.5 m: the dissolution of calcite and feldspar with the precipitation of secondary quartz; (b) F25, 2998.5 m: the leached feldspar and associated secondary minerals; (c) G351, 2444.5 m: feldspar dissolution and Fe-calcite and ankerite precipitation; (d) G351, 2447 m: the leached feldspar and associated secondary minerals, and the secondary intragranular pore is destroyed by ankerite precipitation; (e) F1, 3314.6 m: the precipitation of secondary quartz mineral with a width of approximate 40μm; (f) F104, 3038.9 m: the leached feldspar and associated quartz overgrowths; (g) G891, 2808.4 m: early calcite cement and late ankerite cement; (h) G351, 2444.5 m: the dissolution of calcite and feldspar accompanied by clay minerals, and ankerite cement; (i) F1, 3319.1 m: the intergranular pores are destroyed by ankerite cements. Note: Qo: quartz overgrowth, R: rock fragment, Fd: feldspar dissolution, Cc: calcite, Fc: ferrocalcite, and An: ankerite.
(a)(b)(c)(d)(e)(f)(g)(h)(i)Figure 5
SEM-BSE images of beach-bar sandstones in the Boxing Sag. (a) F1, 3314.6 m: authigenic microquartz (Mq) and a few clay minerals; (b) F1, 3314.6 m: authigenic albite (Ab); (c) G351, 2455 m: the feldspar dissolution is accompanied by the precipitation of illite (yellow arrow); (d) G351, 2455 m: barite (yellow arrow) and pyrite (Py) are filled among particles; (e) F1, 3314.6 m: the leached detrital grain associated with chlorite (yellow arrow), and red spot represents an EDS analyzing point; (f) EDS-tested composition of the barite (BaSO4).
(a)(b)(c)(d)(e)(f)


### 4.2.2. Carbonate Diagenesis

Three types of carbonate cements dominated by calcite, Fe-calcite, and ankerite could be distinguished in the sandstone reservoirs. Different types of carbonate cements could be formed in different periods during the diagenesis process and indicate the pore water characteristics. Calcites occupied the primary pore spaces among clastic grains, displayed the dissolved feature, and showed yellow luminescence (Figures4(g), 4(f), 6(a), and 6(b)). Generally, sandstones containing calcite cements were normally supported by clastic grains with point contacts or exhibited floating structures (Figure 4(h)). Fe-calcites with dark red luminescence filled the intergranular pores and secondary intragranular pores of the dissolved feldspars (Figures 4(c), 6(c), and 6(d)). Ankerites with dark luminescence occupied the intergranular pores and exhibited euhedral rhombs growing in the dissolved feldspar pores and replacing the preexisting calcite (Figures 4(d), 4(h), and 4(i)).Figure 6
Cathodoluminescence (CL) observation of carbonate cements. (a, b) F1, 3319.1 m: calcite (Cc) and ankerite show the yellow and dark luminescence, respectively; (c, d) F104, 3059.4 m: the dissolution of feldspar (F) and Fe-calcite show the dark red luminescence.
(a)(b)(c)(d)


### 4.2.3. Clay and Other Minerals

The observation conducted on thin sections showed that feldspar dissolution was accompanied with clay mineral precipitation. SEM analysis revealed the presence of clay minerals with fibrous and flaky features in feldspar dissolution pores and grew together with minor amounts of microcrystalline authigenic quartz (Figures5(a) and 5(c)). Needle-shaped chlorite could be observed in the dissolved pores (Figure 5(e)). X-ray diffraction data of bulk rocks showed that the mixed-layer illite/smectite and kaolinite, followed by illite and chlorite, are the clay minerals found in majority in the Boxing sandstone reservoirs (Figure 7). The content of mixed-layer illite/smectite decreased at 1750 to 2600 m and then increased from 2600 to 3250 m. However, the mixed-layer ratio (S% in I/S) apparently decreased as the depth increased. The content of kaolinite increased at 1750 to 2600 m and decreased at 2600 to 3250 m as the depth increased. The content of chlorite did not exceed 25% and hardly varied in the vertical distribution.Figure 7
Vertical distribution characteristics of clay minerals in the Boxing Sag.Besides, barite (BaSO4) exhibiting an irregular shape filled among the clastic grain gaps and could be identified via the SEM-EDS analysis in the wells F1 and G351 (Figures 5(d)–5(f)). Pyrite comprised of nodule-shaped aggregates and occurred as a variant of pore-filling cement (Figure 5(d)).


## 4.2.1. Feldspar Diagenesis

Feldspars, including K-feldspars and plagioclases, were partly to fully dissolved in the beach-bar sandstones, which was associated with the precipitation of authigenic quartz and clay minerals (Figures4(a) and 4(b)). The internal fabric of the partly dissolved feldspar could still be applied to distinguish among the composition of inherited minerals (Figures 4(b)–4(d)). On the whole, the secondary intragranular pores resulting from the dissolution of detrital feldspars as well as the primary intergranular pores were filled with newly formed minerals. Microscopy and SEM analysis showed that authigenic quartz mainly existed as quartz overgrowths and microquartz (Figures 4(e), 4(f), and 5(a)). The former was usually observed on the margin of quartz grains whose thickness could reach approximately 30 μm. Actually, quartz cements with exceptionally fine grains were difficult to identify in the sandstone (Figure 4(e)). A large number of microquartz crystals of only a few microns in size filled the gaps between the grains. Moreover, authigenic feldspar (albite) was also generated as overgrowths and well-crystallized grains under the SEM (Figure 5(b)), but it was not as common as authigenic quartz.Figure 4
Photomicrographs of carbonate cements, dissolved feldspars and secondary minerals in thin sections. (a) F1, 3321.5 m: the dissolution of calcite and feldspar with the precipitation of secondary quartz; (b) F25, 2998.5 m: the leached feldspar and associated secondary minerals; (c) G351, 2444.5 m: feldspar dissolution and Fe-calcite and ankerite precipitation; (d) G351, 2447 m: the leached feldspar and associated secondary minerals, and the secondary intragranular pore is destroyed by ankerite precipitation; (e) F1, 3314.6 m: the precipitation of secondary quartz mineral with a width of approximate 40μm; (f) F104, 3038.9 m: the leached feldspar and associated quartz overgrowths; (g) G891, 2808.4 m: early calcite cement and late ankerite cement; (h) G351, 2444.5 m: the dissolution of calcite and feldspar accompanied by clay minerals, and ankerite cement; (i) F1, 3319.1 m: the intergranular pores are destroyed by ankerite cements. Note: Qo: quartz overgrowth, R: rock fragment, Fd: feldspar dissolution, Cc: calcite, Fc: ferrocalcite, and An: ankerite.
(a)(b)(c)(d)(e)(f)(g)(h)(i)Figure 5
SEM-BSE images of beach-bar sandstones in the Boxing Sag. (a) F1, 3314.6 m: authigenic microquartz (Mq) and a few clay minerals; (b) F1, 3314.6 m: authigenic albite (Ab); (c) G351, 2455 m: the feldspar dissolution is accompanied by the precipitation of illite (yellow arrow); (d) G351, 2455 m: barite (yellow arrow) and pyrite (Py) are filled among particles; (e) F1, 3314.6 m: the leached detrital grain associated with chlorite (yellow arrow), and red spot represents an EDS analyzing point; (f) EDS-tested composition of the barite (BaSO4).
(a)(b)(c)(d)(e)(f)


## 4.2.2. Carbonate Diagenesis

Three types of carbonate cements dominated by calcite, Fe-calcite, and ankerite could be distinguished in the sandstone reservoirs. Different types of carbonate cements could be formed in different periods during the diagenesis process and indicate the pore water characteristics. Calcites occupied the primary pore spaces among clastic grains, displayed the dissolved feature, and showed yellow luminescence (Figures4(g), 4(f), 6(a), and 6(b)). Generally, sandstones containing calcite cements were normally supported by clastic grains with point contacts or exhibited floating structures (Figure 4(h)). Fe-calcites with dark red luminescence filled the intergranular pores and secondary intragranular pores of the dissolved feldspars (Figures 4(c), 6(c), and 6(d)). Ankerites with dark luminescence occupied the intergranular pores and exhibited euhedral rhombs growing in the dissolved feldspar pores and replacing the preexisting calcite (Figures 4(d), 4(h), and 4(i)).Figure 6
Cathodoluminescence (CL) observation of carbonate cements. (a, b) F1, 3319.1 m: calcite (Cc) and ankerite show the yellow and dark luminescence, respectively; (c, d) F104, 3059.4 m: the dissolution of feldspar (F) and Fe-calcite show the dark red luminescence.
(a)(b)(c)(d)


## 4.2.3. Clay and Other Minerals

The observation conducted on thin sections showed that feldspar dissolution was accompanied with clay mineral precipitation. SEM analysis revealed the presence of clay minerals with fibrous and flaky features in feldspar dissolution pores and grew together with minor amounts of microcrystalline authigenic quartz (Figures5(a) and 5(c)). Needle-shaped chlorite could be observed in the dissolved pores (Figure 5(e)). X-ray diffraction data of bulk rocks showed that the mixed-layer illite/smectite and kaolinite, followed by illite and chlorite, are the clay minerals found in majority in the Boxing sandstone reservoirs (Figure 7). The content of mixed-layer illite/smectite decreased at 1750 to 2600 m and then increased from 2600 to 3250 m. However, the mixed-layer ratio (S% in I/S) apparently decreased as the depth increased. The content of kaolinite increased at 1750 to 2600 m and decreased at 2600 to 3250 m as the depth increased. The content of chlorite did not exceed 25% and hardly varied in the vertical distribution.Figure 7
Vertical distribution characteristics of clay minerals in the Boxing Sag.Besides, barite (BaSO4) exhibiting an irregular shape filled among the clastic grain gaps and could be identified via the SEM-EDS analysis in the wells F1 and G351 (Figures 5(d)–5(f)). Pyrite comprised of nodule-shaped aggregates and occurred as a variant of pore-filling cement (Figure 5(d)).


## 4.3. Petrophysical Characteristics

The Shahejie Formation sandstone samples in the Boxing Sag exhibited widely distributed porosity and permeability ranging from 1.2% to 32.7% and from 0.023 to 1276 mD as well as from 2.6% to 28.0% and from 0.007 to 152.28 mD, respectively. Generally, the sample porosity and permeability decreased as the burial depth increased from 1500 to 3500 m (Figures8(a) and 8(b)). Based on the reservoir classification from Zeng and Li [36], 34.8% and 48.7% of the Es3 and Es4 sandstones, respectively, were low-porosity reservoirs; their porosity was less than 15.0% (Figure 8(c)); 87.2% and 82.7% of the Es3 and Es4 sandstones, respectively, were low-permeability reservoirs; their permeability was less than 50.0 mD (Figure 8(d)).Figure 8
Petrophysical properties of sandstones in the Es3 and Es4 Formation in the Boxing Sag. (a, b) Vertical distribution of porosity and permeability. (c, d) Histogram distribution of porosity and permeability; the red dash lines distinguish low-porosity and low-permeability reservoirs.The high-pressure mercury intrusion (HPMI) analysis of four beach-bar sandstone samples also satisfied the characteristics of low-porosity and low-permeability sandstone reservoirs. In particular, the permeability was usually less than 1 mD. The distribution of pore throat radius mainly ranged between 0.01 and 1μm depending on the micropore size (Figure 9).Figure 9
Typical pore throat radius distribution obtained from the HPMI experiment.


## 4.4. Fluid Inclusions

Fluid inclusions in authigenic minerals (quartz overgrowth and carbonate) could provide information about the diagenetic environment. Nevertheless, quartz overgrowths could not be easily identified as the grain sizes were dominated by very fine sand in certain wells, and the size of two-phase fluid inclusions in the quartz overgrowths was mainly less than 6μm (Figures 10(a)–10(c)). Together, these factors posed great challenges to the measurement of the homogenization temperature. Herein, the adjacent wells and samples of similar depth were selected for measuring the Th (°C) of aqueous inclusions (Table 2). The Th (°C) of quartz overgrowths mainly ranged between 99°C and 129°C in the Es3x Formation (Figure 11(a)). The Th (°C) from well G351 ranged between 106°C and 121°C in the Es4s Formation (Figure 11(b)). Meanwhile, the fluid inclusions within carbonate cements of wells F104 and F25 were extremely small and rarely found. The Th (°C) mainly ranged between 118°C and 126°C in the Es3 Formation (Figures 10(d) and 11(a)).Figure 10
Petrography of fluid inclusions within quartz overgrowths (Qo) and carbonate cementation (Cc) in sandstones.
(a)(b)(c)(d)Table 2
Microthermometric data of fluid inclusions in the authigenic minerals.
WellDepth (m)StrataHost mineralTh (°C)WellDepth (m)StrataHost mineralTh (°C)F252998.5Es3Qo113F1823109.5Es3Qo115.7F252998.5Es3Qo129F1823109.5Es3Qo116.8F252998.5Es3Qo117F1823109.5Es3Qo111.1F252998.5Es3Qo116G3512444.45Es4Qo106F252998.5Es3Qo116G3512444.45Es4Qo105F1043038.9Es3Qo110G3512444.45Es4Qo115F1043038.9Es3Qo115G3512444.45Es4Qo121F1043038.9Es3Qo120G3512444.45Es4Qo108F1043038.9Es3Qo109G3512444.45Es4Qo113F1043038.9Es3Qo99F252998.5Es3Cc118F1043038.9Es3Qo102F252998.5Es3Cc121F1043038.9Es3Qo111F252998.5Es3Cc119F1823109.5Es3Qo124.1F252998.5Es3Cc119F1823109.5Es3Qo108.3F252998.5Es3Cc121F1823109.5Es3Qo120.7F1043038.9Es3Cc123F1823109.5Es3Qo117.9F1043038.9Es3Cc126F1823109.5Es3Qo106.8Qo: quartz overgrowth; Cc: carbonate cementation.Figure 11
Histogram of Th for fluid inclusions in the quartz overgrowths and carbonate cements. (a) Es3 Formation; (b) Es4 Formation.
(a)(b)


## 4.5. Geochemical Characteristics

The carbon and oxygen isotopic compositions of carbonate cements in the Es4 Formation sandstones show that theδ18O values range between −11.7‰ and −8.4‰, and the δ13C values range between −1.7‰ and −0.5‰. The isotopic δ18O and δ13C values of carbonate cements in the Es3x Formation sandstone range between −12.8‰ and −9.5‰ and between 1.6‰ and 3.3‰, respectively (Table 3).Table 3
Mineralogical and isotopic composition of carbonate. Ca: calcite; Fc: Fe-calcite; An: ankerite.
WellLithologyDepthStrataCarbonate contentMineralsδ18O−PDB (‰)δ13C−PDB (‰)F1Sandstone3321.5Es414.2%70%An+30%Ca-11.3-0.8F1Sandstone3319.1Es413.6%100%An-9.6-0.5F1Sandstone3314.6Es47.4%80%An+20%Ca-11.7-1.1F1Sandstone3312.3Es48.9%80%An+20%Ca-11.4-1.2F1Sandstone3310.3Es43.4%100%An-10-0.8F1Sandstone3311.3Es43.7%100%An-10.3-1G893Sandstone3210.2Es4—95%An+5%Ca-8.4-0.3G893Sandstone3281.0Es425.1%90%An+10%Ca-9.3-1.7F31Sandstone2934.0Es34.6%100%An-12.13F25Sandstone2901.5Es310.2%90%Fc+10%Ca-12.83.3F25Sandstone2998.5Es32.8%90%Fc+10%Ca-13.81.6F104Sandstone3038.9Es316.2%95%An+5%Fc-13.43.3F104Sandstone3039.2Es314.1%95%An+5%Fc-9.52.9The EPMA analysis was conducted to investigate the chemical differences between detrital and authigenic quartz as well as carbonate cements. The results obtained from this analysis of quartz particles showed that CaO and Al2O3 were slightly enriched in authigenic quartz content compared with the detrital phase. Moreover, the chemical compositions of quartz overgrowths at the inner and outer points exhibited no obvious differences (Table 4). The calcite normally displayed a high content in MnO. Fe-calcite and ankerite always had higher content of FeO and/or MgO and a slightly higher content of SrO, Na2O, Al2O3, and K2O than calcite (Table 5).Table 4
Electronic probe microanalysis for quartz in the Es3 sandstone (wt%).
WellDepth (m)PointMgONa2OFeOCaOAl2O3MnOK2OSrOTiO2SiO2TotalF312934.0Q000.030.0200.0200.33099.399.7Qo00.030.020.030.14000.330.0298.699.17Qo0000.050.17000.27098.498.89Q000.0200.0700.030.340.0299.2699.74Qo0000.050.1400.020.290.0299.2399.75Qo0000.020.0500.010.290.0499.0399.44F252998.5Q0.030.02000000.270.0499.4699.82Qo0.0200.040.110.19000.36098.5899.3Qo0.05000.250.200.020.37098.3899.27F1043039.2Q0.020.0400.040.04000.36099.53100.03Qo00.0200.030.18000.29098.999.42Qo0000.080.090.0300.35098.6499.19Q00.03000.02000.29099.1999.53Qo0000.020.17000.35098.899.34Qo00.040.020.050.1200.020.3099.1699.71Table 5
Electronic probe microanalysis for carbonate cements in the sandstone (wt%).
WellDepth (m)MgONa2OFeOCaOAl2O3MnOK2OSrOTiO2Cr2O3CO2TotalF13314.60.270.000.1653.890.031.440.000.040.000.0043.6799.500.250.000.1453.580.031.650.000.000.030.0043.5299.208.990.0015.0630.890.040.540.020.100.000.0043.7399.378.440.0316.6930.240.020.400.000.000.030.0043.4999.34F13311.30.390.001.7053.610.020.360.150.110.000.0043.91100.250.290.020.0554.500.060.700.000.000.000.0043.6799.298.620.1316.3130.770.000.270.040.030.000.0043.87100.048.980.0014.2931.780.040.420.060.270.000.0244.0099.86F3129349.030.0313.5632.690.000.350.030.250.000.0044.20100.149.540.0313.2132.020.000.370.000.110.030.0043.9999.30F252998.50.210.030.5354.790.000.030.030.000.000.0243.6699.300.160.000.5154.700.030.030.020.000.000.0243.5098.970.340.102.2152.840.040.220.000.000.000.0043.7499.490.260.091.7553.170.030.280.010.000.020.0043.5899.18F252901.50.540.001.9253.550.180.170.000.000.000.0044.25100.610.540.042.5652.810.020.200.020.000.000.0043.83100.01F1043038.99.020.0015.5030.840.170.200.070.220.000.0244.12100.160.470.181.3252.700.070.140.070.790.000.0043.3699.100.370.191.2553.550.050.140.030.770.000.0043.85100.200.350.001.2453.300.050.120.000.760.000.0043.4499.260.680.101.2152.510.080.110.090.860.000.0043.3598.990.690.041.1353.300.080.120.060.740.000.0043.86100.029.150.0012.7132.970.000.340.000.280.000.0044.0299.47F1043039.20.390.001.6253.490.020.240.000.100.000.0043.6299.480.310.041.4253.840.000.170.130.220.000.0043.7699.89The REE data of carbonate cements and mudstones are shown in Table6, displaying a high content of light REE (LREE) and a low content of heavy REE (HREE). The REE concentrations have been normalized by chondrite from Boynton [37] and given the subscript N. The δCe and δEu values are calculated by 2CeN/LaN+PrN and 2EuN/SmN+GdN, respectively. The δCe value of carbonate cement and mudstone ranged from 0.38 to 1.08 and from 0.87 to 0.94, with average values of 0.81 and 0.90, respectively. The δEu value of carbonate cement ranged between 0.14 and 2.63, with an average value of 1.10. It had a relatively wider distribution than that of mudstone whose δEu value ranged between 0.51 and 0.61.Table 6
The REE data of carbonate cement and mudstone (μg/g).
REEF25: 2901.5 m (n=3)F25: 2998.5 m (n=4)F104: 3039.2 m (n=4)F104: 3059.4 m (n=3)F1: mudstone (n=4)La20.193.1036.072.832.206.376.818.140.766.995.286.029.1928.1149.3052.3048.1055.60Ce34.745.0360.586.431.7317.2719.5513.300.957.306.1213.194.9239.1290.2099.1084.0094.90Pr4.430.784.930.800.212.452.771.450.060.730.512.000.333.6010.8011.409.2211.10Nd17.783.4513.684.391.0510.4113.495.310.202.502.209.901.9311.7940.8045.8033.4042.80Sm3.790.674.501.140.432.904.120.590.050.170.442.970.471.386.937.554.666.30Eu1.410.121.120.380.260.541.190.430.000.240.100.910.180.391.341.390.851.00Gd4.721.054.111.010.411.733.750.980.040.420.332.100.271.016.206.234.585.32Tb0.480.030.410.270.040.351.000.140.010.050.080.500.060.191.011.040.820.89Dy2.550.152.591.530.502.075.750.680.050.350.523.300.401.035.475.504.554.92Ho0.520.120.600.310.080.441.010.140.010.110.090.740.120.251.001.030.970.89Er1.670.281.720.780.221.202.770.540.050.180.342.200.050.672.943.063.042.60Tm0.32<0.00.150.150.040.160.330.060.000.020.070.33<0.00.030.470.470.480.41Yb1.040.060.710.660.230.961.930.340.050.160.292.050.320.563.143.333.343.16Lu0.080.030.170.080.030.140.260.050.010.030.040.300.040.110.430.450.490.40ΣREE93.7314.86131.3320.757.4246.9764.7332.172.2419.2516.4046.5218.2688.23220.02238.66198.49230.28LREE82.3413.15120.8815.975.8739.9347.9329.222.0117.9314.6535.0017.0184.38199.37217.54180.23211.70HREE11.391.7210.454.781.547.0416.802.950.221.321.7511.521.253.8520.6521.1218.2618.58δCe0.850.760.961.020.481.051.080.860.810.630.710.910.380.810.900.940.900.87δEu1.020.430.781.061.880.680.911.710.142.630.781.071.390.960.610.600.550.51


## 5. Discussions

### 5.1. Diagenetic Sequences

The diagenetic processes of beach-bar sandstone reservoirs can be elucidated by investigating the textural relationship through petrological observations. First, rock particles normally displayed point contacts and a floating structure, indicating weak compaction when early-stage calcite filled the intergranular pores (Figures4(a), 4(g), and 4(h)). However, the content of early-stage calcite cement was relatively low in thin sections. Second, calcite and feldspar dissolutions were accompanied with authigenic mineral precipitations within reservoirs, which is supported by quartz overgrowths and kaolinite that are normally observed near dissolved feldspar and that occupy the intergranular pores (Figures 4(b), 4(d), and 4(f)). The compaction further destroyed the pore spaces of reservoirs and was controlled by different burial history owing to the particles being dominated by line to concavo-convex contacts. Moreover, K-feldspar reacted with kaolinite and smectite was converted into illite in reservoirs, thereby promoting the formation of mixed-layer illite/smectite or illite during progressive burial [12, 38]. Thus, the illite content gradually increased whereas the kaolinite content began to decrease at approximately 2600 m. The mixed-layer ratios (S% in I/S) of illite/smectite decreased as the depth increased (Figure 7). Finally, late-stage Fe-calcite and ankerite formed as dominant pore-filling cements, occupying the intergranular and intragranular pores and growing around the euhedral quartz overgrowth (Figures 4(c), 4(d), and 4(i)).In summary, beach-bar sandstone reservoirs in the Boxing Sag mainly experienced compaction and calcite cementation in the early stage; calcite and feldspar dissolution were accompanied with the precipitation of quartz and kaolinite as well as clay minerals conversion; and Fe-calcite and ankerite cementation occurred in the late stage (Figure12).Figure 12
Burial and diagenetic history of the Es3x Formation sandstone reservoirs, modified from [27, 29].


### 5.2. Origin of Cementation

#### 5.2.1. Quartz Cementation

The origin of silica of quartz cements in the sandstone reservoirs can be divided into internal and external sources [25, 39]. Internal sources normally comprise feldspar and rock fragment dissolution, clay mineral reaction, pressure solution of quartz particles, and biogenic silica [26, 40–42]. External sources generally include the transport of deep fluids [43, 44].Quartz cements are unlikely to stem from biogenetic silica because the sandstones being study are sediments deposited in a lacustrine environment rather than in a marine environment. Petrography analysis also shows no evidence of the existence of biological silicon materials. Additionally, Wang et al. [21, 22] reported that the silica sources for quartz overgrowths were mainly influenced by hydrothermal fluids in the Permian Upper Shihezi Formation sandstones at the Qingcheng Rise, which is approximately only 15 km away from the wells in the study area (Figure 1), because the Th (°C) of aqueous inclusions was higher than its maximum burial temperature, δEu anomaly, and the enrichment of several trace elements in quartz overgrowths. However, quartz overgrowths of samples herein do not appear abnormally high Th value of aqueous inclusions and the presence of different of major elements (Figures 11 and 13). The pressure dissolution of detrital quartz grains possibly provides little internal silica source owing to the particles that are dominated by a point-to-line contact in the Es3x sandstone. Thus, the silica sources of authigenic quartz primarily originate from the clay mineral reactions and feldspar and rock fragment dissolutions.Figure 13
EPMA analysis of detrital quartz and quartz overgrowth (Qo) in the Es3x interval. (a, c, e, g, i) BSE images showing the EPMA analysis position. (b, d, f, h, j) Elemental composition characteristics in detrital quartz and Qo.
(a)(b)(c)(d)(e)(f)(g)(h)(i)(j)The volcanic rock fragments are distributed in the Shahejie Formation beach-bar sandstones and easily transformed into smectite within reservoirs during the early diagenesis ([25]; Figure 7). During progressive diagenesis, the conversion reaction of smectite to illite mainly occurs at approximately 70°C–100°C, which probably provides a certain amount of silica for the precipitation of quartz [38, 41]. Petrographic observations show the precipitation of authigenic microquartz grains growing together with the clay minerals and the content of illite increasing as the burial depth increases. These results support the generation of quartz cement was associated with the conversion of smectite.Furthermore, petrographic observations show that the generation of authigenic quartz overgrowths was normally accompanied with feldspar dissolution, which could be an origin for quartz cementation. In addition to the ion concentration, the pH, temperature and pressure, chemical composition, and structure of plagioclase are key factors determining the dissolution or precipitation process. This is based on thermodynamic calculations that show the solubility of plagioclase increases as the calcium content increases [45]. Therefore, the dissolution of early calcite and feldspars probably leads to the enrichment of Ca2+, followed by Na+ and K+ in the pore water. The Al3+ widely existed in the reaction process of aluminosilicate minerals [12]. The numerical simulations indicated that the silica formed by feldspar dissolution is locally precipitated in the deep burial process, which can be further proved by a positive relationship between the content of feldspar dissolution pores and quartz cement (Figure 14; [33]).Figure 14
Relationship between the content of feldspar dissolution pores and quartz cement.


#### 5.2.2. Carbonate Cementation

Carbonate minerals as cements are universal and normally occupy the pore space of sandstone samples. Petrographic and EPMA analyses reveal the presence of calcite, Fe-calcite, and ankerite. The signals of major elements and the REE content of carbonate cements probably provide the clues about the origin of late Fe-calcite and ankerite. The external sources include the precipitation of carbonate from meteoric water, adjacent mudstones, and deep fluids [8, 31]. Internal sources include the dissolution of detrital carbonate grains, early carbonate, and unstable compositions as well as the conversion of clay minerals [46].The late-stage Fe-calcite and ankerite minerals not only contain higher amounts of FeO and MgO (Figure15) but also contain slightly higher amounts of SrO, Na2O, Al2O3, and K2O compared with calcite (Figure 16). The calcite with high MnO content formed in the early stage is mainly influenced by mudstone [17, 31]. Mn-oxide reduction by organic matter at low temperatures could result in the enrichment of Mn2+ in calcite that showed bright yellow luminescence [47]. The Th (°C) of late-stage carbonate cements exceeds 115°C, suggesting that the organic matter has already discharged a large amount of organic acids and CO2, which contributed to the dissolution of feldspars and early calcites as well as the reprecipitation of late carbonate. Additionally, the persistent conversion of clay minerals also supplies abundant cations in the pore water. Thus, the ions (Ca2+, Fe2+, Mg2+, Na+, K+, and Al3+) for the formation of late Fe-calcites and ankerites were probably derived from the dissolution of preexisting minerals and the conversion of clay minerals locally. Besides, previous research indicated that the micritic carbonate within mudstones in the Dongying Depression exhibited a high content of Sr2+ [14], which gradually entered into pore water, resulting in a high SrO content in late-stage carbonate. The presence of barite was normally associated with hydrothermal fluid [21, 22]. The barite mineral has markedly low solubility, whereas barium is common within the organic matter [48, 49]. The dissolution of gypsum within mudstone provided sulfate into pore water to promote the precipitation of barite [50].Figure 15
Ternary diagrams showing normalized compositions of carbonate cement from EPMA analysis in wt%.Figure 16
Major elements of carbonate cement from EPMA analysis. (a) F1 well; (b) F31 well; (c) F25 well; and (d) F104 well.
(a)(b)(c)(d)The REE signature reflects whether the external meteoric water and deep fluids are involved in the formation of carbonate cements. The mudstones in the study area were normally enriched in LREE content and demonstrated HREE depletion as well as a slight negative anomaly in theδEu value (Figure 17(a)). The late-stage carbonate cements typically demonstrated similar REE patterns because the recrystallization of carbonate can cause a variety in total REE content (ΣREE) rather than variable REE patterns (Figures 17(b) and 17(c)). The index of the δCe value can reveal the impact of meteoric water [51, 52]. The δCe values of late carbonate cements have an average of 0.81, which is close to the δCe values of mudstones, and do not show obvious anomaly. Moreover, the δEu anomalies are utilized to assess the impact of hydrothermal fluids as the Eu is enriched in highly reducing hydrothermal fluids [53]. The late-stage carbonate cements demonstrate significantly fluctuations in the δEu values, with an average of 1.10, which is larger than the δEu values of mudstones and displays a slightly positive Eu anomaly, which probably reveals that hydrothermal fluids are involved in the precipitation of late carbonate [54]. However, the Th (°C) of late-stage carbonate ranges between 118°C and 126°C, which indicates a normal burial condition and is inconsistent with the hydrothermal fluid source (Figure 12). The feldspars dissolution, particularly plagioclases with a high calcium content, which provides divalent Eu into pore water owing to the divalent Eu, tends to enter the crystal lattice of plagioclase and results in increased δEu values within late carbonate in the reducing environment [19, 55]. Therefore, the formation of late carbonate cements is mainly influenced by the carbonate signature within mudstone owing to the similar REE patterns. Unstable mineral dissolution and clay mineral conversion result in ions being supplied to pore water, changing the major and trace elements within late-stage carbonate.Figure 17
Spider diagram of the pattern of rare earth element (REE). Chondrite-normalized REE patterns in (a) mudstones and data from Bai et al. [14] and in carbonate cements within Es3x interval from (b) F25 and (c) F104 wells, respectively.
(a)(b)(c)


### 5.3. Diagenetic Fluid Transformation and Evolution

The petrological features demonstrated that beach-bar sandstone reservoirs experienced early-stage calcite cementation, calcite and feldspar dissolution with the precipitation of quartz and kaolinite, and late-stage cementation for Fe-calcite and ankerite. The Th (°C) of fluid inclusion provides more detailed information about the evolution of diagenetic fluids. The Th (°C) of quartz overgrowths and late carbonate cements in the Es3x sandstone range from 99°C to 129°C and from 118°C to 126°C, respectively, and the Th (°C) of quartz overgrowths of well G351 in the Es4s sandstone ranges from 106°C to 121°C (Figure11). These Th (°C) values are similar to the previous results in quartz overgrowths (90°C to 120°C) and late-stage carbonate cementation (115°C to 135°C; [27]). They indicate that the impact of acidic fluid probably begins at ~90°C and continues until ~115°C.The precipitation of early-stage calcite among intergranular pores is probably affected by the ions resulting from mudstone compaction in an alkaline environment. The biodegradation of oils requires the participation of aerobic bacteria and oxidants carried by meteoric water and can produce organic acids to dissolve minerals within reservoir [56]. However, beach-bar sandstone reservoir is continuously buried based on the burial history, rather than tectonic uplift (Figure 12). Additionally, fluid overpressure is developed (Figure 1(c)), and the by-products from feldspar dissolution can always be observed nearby and generally obeys the principle of mass balance in a closed system (Figure 14; [6, 33]), which indicate that meteoric water may have little effect on the dissolution of minerals in the reservoirs. Thus, the thermal degradation of kerogen within mudstone discharges an acidic fluid into the reservoirs to dissolve the preexisting calcite and feldspar, which provide major silica sources for the growth of authigenic quartz. The formation of late-stage Fe-calcite and ankerite minerals are mainly influenced by mudstone fluids formed in alkaline conditions, based on the Th (°C) of fluid inclusions and major and trace elements signature. Moreover, the C–O isotopes of carbonate cements represent the thermal evolution of organic matter and provide additional information about diagenetic fluids [57]. δ13C and δ18O of micritic carbonate within mudstone possibly reflect the carbonate characteristics during the sedimentary period. Their averages are 3.5% and −9.5%, respectively [14]. The negative shift of δ18O within late carbonate cement indicates the higher temperature of precipitation because δ18O is sensitive to the diagenetic temperature [58]. The δ13C value is deemed an effective index for organic–inorganic interaction in the diagenetic process [59] and is associated with preexisting carbonate dissolution, bacterial sulfate reduction, microbial degradation of organic matter, and thermal decarboxylation of hydrocarbons [60, 61]. The similar distribution of δ13C values in micritic carbonate and late-stage carbonate cements within the Es3x sandstone indicates that the fluid for late-stage carbonate cements mainly originate from micritic carbonate and preexisting calcite. Conversely, the Es4s sandstone experiences a longer burial process and the decarboxylation of organic matter, which contributes to carbonate cements having negative δ13C values that are obviously lower than that of the Es3x sandstone and micritic carbonate (Figure 18). Thus, beach-bar sandstone reservoirs in the Boxing Sag generally evolved from being alkaline to acidic to alkaline. The acidic environment probably lasted for approximately 27 Ma (from ~30 Ma to ~3 Ma) and 28 Ma (from ~32 Ma to ~4 Ma) in the Es3x and Es4s sandstones, respectively (Figure 12).Figure 18
Carbon and oxygen isotopic compositions of carbonate cements and micritic carbonate (red box) within mudstone from Bai et al. [14].


### 5.4. Impacts on the Reservoir Quality

Sandstones in the research area are characterized by the general proportion of low-porosity and high proportion of low-permeability reservoirs (Figure8), which probably implies that the sandstone reservoirs exhibit complex pore structures and heterogeneity. HPMI results also indicate that beach-bar sandstone samples are dominated by micropores, which increase the complexity of pore throat structures and decrease the permeability of sandstone reservoirs. The original depositional environments and later diagenesis determine the pore structure of sandstones, which significantly helps in maintaining and enhancing oil recovery [1, 62, 63]. The depositional environments include the framework grain compositions, size, sorting, and shape and affect the initial pore space among grains. However, the sandstone samples exhibit similar grain compositions, grain sizes, and sorting coefficient (Table 1), which probably indicate that these sandstones exhibit a slightly different initial porosity. Therefore, diagenetic modifications involving compaction, dissolution, and cementation during the burial process further reshape the pore structure and mainly control the sandstone reservoir quality. The petrographic analysis of samples indicates that compaction has the most negative influence on the reservoir quality (Figure 19). Meanwhile, cementation, particularly the content of carbonate cement, also significantly helps in reducing the reservoir quality of sandstones in certain samples owing to a negative correlation between the plane porosity and carbonate cements (Figure 20(a)). Previous researches have also proved that the distance to the sandstone–mudstone contact normally controls the precipitation of early-stage calcite. However, the carbonate in this research mostly consists of late-stage Fe-calcite and ankerite, which is a product of the water–rock reaction and records the signature of diagenetic fluids. The content of carbonate cementation has a negative relationship with the distance to sandstone–mudstone contact, as well as a slightly negative relationship with porosity and permeability (Figures 20(b) and 21), implying mass balance in a closed system within sandstone reservoirs.Figure 19
Diagram showing the compaction porosity loss versus cementation porosity loss in the sandstone reservoirs [65].Figure 20
Relationship between the content of carbonate cement, plane porosity of thin section, and the distance from sandstone–mudstone contact.
(a)(b)Figure 21
Vertical distribution of plane porosity and carbonate content of thin sections, porosity, and permeability in the F1 well in the Boxing Sag. Point A: all intergranular pores are destroyed by strong carbonate cementation; point B: a small amount of intergranular pores and carbonate cements; point C: intergranular pores are relatively common.


## 5.1. Diagenetic Sequences

The diagenetic processes of beach-bar sandstone reservoirs can be elucidated by investigating the textural relationship through petrological observations. First, rock particles normally displayed point contacts and a floating structure, indicating weak compaction when early-stage calcite filled the intergranular pores (Figures4(a), 4(g), and 4(h)). However, the content of early-stage calcite cement was relatively low in thin sections. Second, calcite and feldspar dissolutions were accompanied with authigenic mineral precipitations within reservoirs, which is supported by quartz overgrowths and kaolinite that are normally observed near dissolved feldspar and that occupy the intergranular pores (Figures 4(b), 4(d), and 4(f)). The compaction further destroyed the pore spaces of reservoirs and was controlled by different burial history owing to the particles being dominated by line to concavo-convex contacts. Moreover, K-feldspar reacted with kaolinite and smectite was converted into illite in reservoirs, thereby promoting the formation of mixed-layer illite/smectite or illite during progressive burial [12, 38]. Thus, the illite content gradually increased whereas the kaolinite content began to decrease at approximately 2600 m. The mixed-layer ratios (S% in I/S) of illite/smectite decreased as the depth increased (Figure 7). Finally, late-stage Fe-calcite and ankerite formed as dominant pore-filling cements, occupying the intergranular and intragranular pores and growing around the euhedral quartz overgrowth (Figures 4(c), 4(d), and 4(i)).In summary, beach-bar sandstone reservoirs in the Boxing Sag mainly experienced compaction and calcite cementation in the early stage; calcite and feldspar dissolution were accompanied with the precipitation of quartz and kaolinite as well as clay minerals conversion; and Fe-calcite and ankerite cementation occurred in the late stage (Figure12).Figure 12
Burial and diagenetic history of the Es3x Formation sandstone reservoirs, modified from [27, 29].


## 5.2. Origin of Cementation

### 5.2.1. Quartz Cementation

The origin of silica of quartz cements in the sandstone reservoirs can be divided into internal and external sources [25, 39]. Internal sources normally comprise feldspar and rock fragment dissolution, clay mineral reaction, pressure solution of quartz particles, and biogenic silica [26, 40–42]. External sources generally include the transport of deep fluids [43, 44].Quartz cements are unlikely to stem from biogenetic silica because the sandstones being study are sediments deposited in a lacustrine environment rather than in a marine environment. Petrography analysis also shows no evidence of the existence of biological silicon materials. Additionally, Wang et al. [21, 22] reported that the silica sources for quartz overgrowths were mainly influenced by hydrothermal fluids in the Permian Upper Shihezi Formation sandstones at the Qingcheng Rise, which is approximately only 15 km away from the wells in the study area (Figure 1), because the Th (°C) of aqueous inclusions was higher than its maximum burial temperature, δEu anomaly, and the enrichment of several trace elements in quartz overgrowths. However, quartz overgrowths of samples herein do not appear abnormally high Th value of aqueous inclusions and the presence of different of major elements (Figures 11 and 13). The pressure dissolution of detrital quartz grains possibly provides little internal silica source owing to the particles that are dominated by a point-to-line contact in the Es3x sandstone. Thus, the silica sources of authigenic quartz primarily originate from the clay mineral reactions and feldspar and rock fragment dissolutions.Figure 13
EPMA analysis of detrital quartz and quartz overgrowth (Qo) in the Es3x interval. (a, c, e, g, i) BSE images showing the EPMA analysis position. (b, d, f, h, j) Elemental composition characteristics in detrital quartz and Qo.
(a)(b)(c)(d)(e)(f)(g)(h)(i)(j)The volcanic rock fragments are distributed in the Shahejie Formation beach-bar sandstones and easily transformed into smectite within reservoirs during the early diagenesis ([25]; Figure 7). During progressive diagenesis, the conversion reaction of smectite to illite mainly occurs at approximately 70°C–100°C, which probably provides a certain amount of silica for the precipitation of quartz [38, 41]. Petrographic observations show the precipitation of authigenic microquartz grains growing together with the clay minerals and the content of illite increasing as the burial depth increases. These results support the generation of quartz cement was associated with the conversion of smectite.Furthermore, petrographic observations show that the generation of authigenic quartz overgrowths was normally accompanied with feldspar dissolution, which could be an origin for quartz cementation. In addition to the ion concentration, the pH, temperature and pressure, chemical composition, and structure of plagioclase are key factors determining the dissolution or precipitation process. This is based on thermodynamic calculations that show the solubility of plagioclase increases as the calcium content increases [45]. Therefore, the dissolution of early calcite and feldspars probably leads to the enrichment of Ca2+, followed by Na+ and K+ in the pore water. The Al3+ widely existed in the reaction process of aluminosilicate minerals [12]. The numerical simulations indicated that the silica formed by feldspar dissolution is locally precipitated in the deep burial process, which can be further proved by a positive relationship between the content of feldspar dissolution pores and quartz cement (Figure 14; [33]).Figure 14
Relationship between the content of feldspar dissolution pores and quartz cement.


### 5.2.2. Carbonate Cementation

Carbonate minerals as cements are universal and normally occupy the pore space of sandstone samples. Petrographic and EPMA analyses reveal the presence of calcite, Fe-calcite, and ankerite. The signals of major elements and the REE content of carbonate cements probably provide the clues about the origin of late Fe-calcite and ankerite. The external sources include the precipitation of carbonate from meteoric water, adjacent mudstones, and deep fluids [8, 31]. Internal sources include the dissolution of detrital carbonate grains, early carbonate, and unstable compositions as well as the conversion of clay minerals [46].The late-stage Fe-calcite and ankerite minerals not only contain higher amounts of FeO and MgO (Figure15) but also contain slightly higher amounts of SrO, Na2O, Al2O3, and K2O compared with calcite (Figure 16). The calcite with high MnO content formed in the early stage is mainly influenced by mudstone [17, 31]. Mn-oxide reduction by organic matter at low temperatures could result in the enrichment of Mn2+ in calcite that showed bright yellow luminescence [47]. The Th (°C) of late-stage carbonate cements exceeds 115°C, suggesting that the organic matter has already discharged a large amount of organic acids and CO2, which contributed to the dissolution of feldspars and early calcites as well as the reprecipitation of late carbonate. Additionally, the persistent conversion of clay minerals also supplies abundant cations in the pore water. Thus, the ions (Ca2+, Fe2+, Mg2+, Na+, K+, and Al3+) for the formation of late Fe-calcites and ankerites were probably derived from the dissolution of preexisting minerals and the conversion of clay minerals locally. Besides, previous research indicated that the micritic carbonate within mudstones in the Dongying Depression exhibited a high content of Sr2+ [14], which gradually entered into pore water, resulting in a high SrO content in late-stage carbonate. The presence of barite was normally associated with hydrothermal fluid [21, 22]. The barite mineral has markedly low solubility, whereas barium is common within the organic matter [48, 49]. The dissolution of gypsum within mudstone provided sulfate into pore water to promote the precipitation of barite [50].Figure 15
Ternary diagrams showing normalized compositions of carbonate cement from EPMA analysis in wt%.Figure 16
Major elements of carbonate cement from EPMA analysis. (a) F1 well; (b) F31 well; (c) F25 well; and (d) F104 well.
(a)(b)(c)(d)The REE signature reflects whether the external meteoric water and deep fluids are involved in the formation of carbonate cements. The mudstones in the study area were normally enriched in LREE content and demonstrated HREE depletion as well as a slight negative anomaly in theδEu value (Figure 17(a)). The late-stage carbonate cements typically demonstrated similar REE patterns because the recrystallization of carbonate can cause a variety in total REE content (ΣREE) rather than variable REE patterns (Figures 17(b) and 17(c)). The index of the δCe value can reveal the impact of meteoric water [51, 52]. The δCe values of late carbonate cements have an average of 0.81, which is close to the δCe values of mudstones, and do not show obvious anomaly. Moreover, the δEu anomalies are utilized to assess the impact of hydrothermal fluids as the Eu is enriched in highly reducing hydrothermal fluids [53]. The late-stage carbonate cements demonstrate significantly fluctuations in the δEu values, with an average of 1.10, which is larger than the δEu values of mudstones and displays a slightly positive Eu anomaly, which probably reveals that hydrothermal fluids are involved in the precipitation of late carbonate [54]. However, the Th (°C) of late-stage carbonate ranges between 118°C and 126°C, which indicates a normal burial condition and is inconsistent with the hydrothermal fluid source (Figure 12). The feldspars dissolution, particularly plagioclases with a high calcium content, which provides divalent Eu into pore water owing to the divalent Eu, tends to enter the crystal lattice of plagioclase and results in increased δEu values within late carbonate in the reducing environment [19, 55]. Therefore, the formation of late carbonate cements is mainly influenced by the carbonate signature within mudstone owing to the similar REE patterns. Unstable mineral dissolution and clay mineral conversion result in ions being supplied to pore water, changing the major and trace elements within late-stage carbonate.Figure 17
Spider diagram of the pattern of rare earth element (REE). Chondrite-normalized REE patterns in (a) mudstones and data from Bai et al. [14] and in carbonate cements within Es3x interval from (b) F25 and (c) F104 wells, respectively.
(a)(b)(c)


## 5.2.1. Quartz Cementation

The origin of silica of quartz cements in the sandstone reservoirs can be divided into internal and external sources [25, 39]. Internal sources normally comprise feldspar and rock fragment dissolution, clay mineral reaction, pressure solution of quartz particles, and biogenic silica [26, 40–42]. External sources generally include the transport of deep fluids [43, 44].Quartz cements are unlikely to stem from biogenetic silica because the sandstones being study are sediments deposited in a lacustrine environment rather than in a marine environment. Petrography analysis also shows no evidence of the existence of biological silicon materials. Additionally, Wang et al. [21, 22] reported that the silica sources for quartz overgrowths were mainly influenced by hydrothermal fluids in the Permian Upper Shihezi Formation sandstones at the Qingcheng Rise, which is approximately only 15 km away from the wells in the study area (Figure 1), because the Th (°C) of aqueous inclusions was higher than its maximum burial temperature, δEu anomaly, and the enrichment of several trace elements in quartz overgrowths. However, quartz overgrowths of samples herein do not appear abnormally high Th value of aqueous inclusions and the presence of different of major elements (Figures 11 and 13). The pressure dissolution of detrital quartz grains possibly provides little internal silica source owing to the particles that are dominated by a point-to-line contact in the Es3x sandstone. Thus, the silica sources of authigenic quartz primarily originate from the clay mineral reactions and feldspar and rock fragment dissolutions.Figure 13
EPMA analysis of detrital quartz and quartz overgrowth (Qo) in the Es3x interval. (a, c, e, g, i) BSE images showing the EPMA analysis position. (b, d, f, h, j) Elemental composition characteristics in detrital quartz and Qo.
(a)(b)(c)(d)(e)(f)(g)(h)(i)(j)The volcanic rock fragments are distributed in the Shahejie Formation beach-bar sandstones and easily transformed into smectite within reservoirs during the early diagenesis ([25]; Figure 7). During progressive diagenesis, the conversion reaction of smectite to illite mainly occurs at approximately 70°C–100°C, which probably provides a certain amount of silica for the precipitation of quartz [38, 41]. Petrographic observations show the precipitation of authigenic microquartz grains growing together with the clay minerals and the content of illite increasing as the burial depth increases. These results support the generation of quartz cement was associated with the conversion of smectite.Furthermore, petrographic observations show that the generation of authigenic quartz overgrowths was normally accompanied with feldspar dissolution, which could be an origin for quartz cementation. In addition to the ion concentration, the pH, temperature and pressure, chemical composition, and structure of plagioclase are key factors determining the dissolution or precipitation process. This is based on thermodynamic calculations that show the solubility of plagioclase increases as the calcium content increases [45]. Therefore, the dissolution of early calcite and feldspars probably leads to the enrichment of Ca2+, followed by Na+ and K+ in the pore water. The Al3+ widely existed in the reaction process of aluminosilicate minerals [12]. The numerical simulations indicated that the silica formed by feldspar dissolution is locally precipitated in the deep burial process, which can be further proved by a positive relationship between the content of feldspar dissolution pores and quartz cement (Figure 14; [33]).Figure 14
Relationship between the content of feldspar dissolution pores and quartz cement.


## 5.2.2. Carbonate Cementation

Carbonate minerals as cements are universal and normally occupy the pore space of sandstone samples. Petrographic and EPMA analyses reveal the presence of calcite, Fe-calcite, and ankerite. The signals of major elements and the REE content of carbonate cements probably provide the clues about the origin of late Fe-calcite and ankerite. The external sources include the precipitation of carbonate from meteoric water, adjacent mudstones, and deep fluids [8, 31]. Internal sources include the dissolution of detrital carbonate grains, early carbonate, and unstable compositions as well as the conversion of clay minerals [46].The late-stage Fe-calcite and ankerite minerals not only contain higher amounts of FeO and MgO (Figure15) but also contain slightly higher amounts of SrO, Na2O, Al2O3, and K2O compared with calcite (Figure 16). The calcite with high MnO content formed in the early stage is mainly influenced by mudstone [17, 31]. Mn-oxide reduction by organic matter at low temperatures could result in the enrichment of Mn2+ in calcite that showed bright yellow luminescence [47]. The Th (°C) of late-stage carbonate cements exceeds 115°C, suggesting that the organic matter has already discharged a large amount of organic acids and CO2, which contributed to the dissolution of feldspars and early calcites as well as the reprecipitation of late carbonate. Additionally, the persistent conversion of clay minerals also supplies abundant cations in the pore water. Thus, the ions (Ca2+, Fe2+, Mg2+, Na+, K+, and Al3+) for the formation of late Fe-calcites and ankerites were probably derived from the dissolution of preexisting minerals and the conversion of clay minerals locally. Besides, previous research indicated that the micritic carbonate within mudstones in the Dongying Depression exhibited a high content of Sr2+ [14], which gradually entered into pore water, resulting in a high SrO content in late-stage carbonate. The presence of barite was normally associated with hydrothermal fluid [21, 22]. The barite mineral has markedly low solubility, whereas barium is common within the organic matter [48, 49]. The dissolution of gypsum within mudstone provided sulfate into pore water to promote the precipitation of barite [50].Figure 15
Ternary diagrams showing normalized compositions of carbonate cement from EPMA analysis in wt%.Figure 16
Major elements of carbonate cement from EPMA analysis. (a) F1 well; (b) F31 well; (c) F25 well; and (d) F104 well.
(a)(b)(c)(d)The REE signature reflects whether the external meteoric water and deep fluids are involved in the formation of carbonate cements. The mudstones in the study area were normally enriched in LREE content and demonstrated HREE depletion as well as a slight negative anomaly in theδEu value (Figure 17(a)). The late-stage carbonate cements typically demonstrated similar REE patterns because the recrystallization of carbonate can cause a variety in total REE content (ΣREE) rather than variable REE patterns (Figures 17(b) and 17(c)). The index of the δCe value can reveal the impact of meteoric water [51, 52]. The δCe values of late carbonate cements have an average of 0.81, which is close to the δCe values of mudstones, and do not show obvious anomaly. Moreover, the δEu anomalies are utilized to assess the impact of hydrothermal fluids as the Eu is enriched in highly reducing hydrothermal fluids [53]. The late-stage carbonate cements demonstrate significantly fluctuations in the δEu values, with an average of 1.10, which is larger than the δEu values of mudstones and displays a slightly positive Eu anomaly, which probably reveals that hydrothermal fluids are involved in the precipitation of late carbonate [54]. However, the Th (°C) of late-stage carbonate ranges between 118°C and 126°C, which indicates a normal burial condition and is inconsistent with the hydrothermal fluid source (Figure 12). The feldspars dissolution, particularly plagioclases with a high calcium content, which provides divalent Eu into pore water owing to the divalent Eu, tends to enter the crystal lattice of plagioclase and results in increased δEu values within late carbonate in the reducing environment [19, 55]. Therefore, the formation of late carbonate cements is mainly influenced by the carbonate signature within mudstone owing to the similar REE patterns. Unstable mineral dissolution and clay mineral conversion result in ions being supplied to pore water, changing the major and trace elements within late-stage carbonate.Figure 17
Spider diagram of the pattern of rare earth element (REE). Chondrite-normalized REE patterns in (a) mudstones and data from Bai et al. [14] and in carbonate cements within Es3x interval from (b) F25 and (c) F104 wells, respectively.
(a)(b)(c)


## 5.3. Diagenetic Fluid Transformation and Evolution

The petrological features demonstrated that beach-bar sandstone reservoirs experienced early-stage calcite cementation, calcite and feldspar dissolution with the precipitation of quartz and kaolinite, and late-stage cementation for Fe-calcite and ankerite. The Th (°C) of fluid inclusion provides more detailed information about the evolution of diagenetic fluids. The Th (°C) of quartz overgrowths and late carbonate cements in the Es3x sandstone range from 99°C to 129°C and from 118°C to 126°C, respectively, and the Th (°C) of quartz overgrowths of well G351 in the Es4s sandstone ranges from 106°C to 121°C (Figure11). These Th (°C) values are similar to the previous results in quartz overgrowths (90°C to 120°C) and late-stage carbonate cementation (115°C to 135°C; [27]). They indicate that the impact of acidic fluid probably begins at ~90°C and continues until ~115°C.The precipitation of early-stage calcite among intergranular pores is probably affected by the ions resulting from mudstone compaction in an alkaline environment. The biodegradation of oils requires the participation of aerobic bacteria and oxidants carried by meteoric water and can produce organic acids to dissolve minerals within reservoir [56]. However, beach-bar sandstone reservoir is continuously buried based on the burial history, rather than tectonic uplift (Figure 12). Additionally, fluid overpressure is developed (Figure 1(c)), and the by-products from feldspar dissolution can always be observed nearby and generally obeys the principle of mass balance in a closed system (Figure 14; [6, 33]), which indicate that meteoric water may have little effect on the dissolution of minerals in the reservoirs. Thus, the thermal degradation of kerogen within mudstone discharges an acidic fluid into the reservoirs to dissolve the preexisting calcite and feldspar, which provide major silica sources for the growth of authigenic quartz. The formation of late-stage Fe-calcite and ankerite minerals are mainly influenced by mudstone fluids formed in alkaline conditions, based on the Th (°C) of fluid inclusions and major and trace elements signature. Moreover, the C–O isotopes of carbonate cements represent the thermal evolution of organic matter and provide additional information about diagenetic fluids [57]. δ13C and δ18O of micritic carbonate within mudstone possibly reflect the carbonate characteristics during the sedimentary period. Their averages are 3.5% and −9.5%, respectively [14]. The negative shift of δ18O within late carbonate cement indicates the higher temperature of precipitation because δ18O is sensitive to the diagenetic temperature [58]. The δ13C value is deemed an effective index for organic–inorganic interaction in the diagenetic process [59] and is associated with preexisting carbonate dissolution, bacterial sulfate reduction, microbial degradation of organic matter, and thermal decarboxylation of hydrocarbons [60, 61]. The similar distribution of δ13C values in micritic carbonate and late-stage carbonate cements within the Es3x sandstone indicates that the fluid for late-stage carbonate cements mainly originate from micritic carbonate and preexisting calcite. Conversely, the Es4s sandstone experiences a longer burial process and the decarboxylation of organic matter, which contributes to carbonate cements having negative δ13C values that are obviously lower than that of the Es3x sandstone and micritic carbonate (Figure 18). Thus, beach-bar sandstone reservoirs in the Boxing Sag generally evolved from being alkaline to acidic to alkaline. The acidic environment probably lasted for approximately 27 Ma (from ~30 Ma to ~3 Ma) and 28 Ma (from ~32 Ma to ~4 Ma) in the Es3x and Es4s sandstones, respectively (Figure 12).Figure 18
Carbon and oxygen isotopic compositions of carbonate cements and micritic carbonate (red box) within mudstone from Bai et al. [14].


## 5.4. Impacts on the Reservoir Quality

Sandstones in the research area are characterized by the general proportion of low-porosity and high proportion of low-permeability reservoirs (Figure8), which probably implies that the sandstone reservoirs exhibit complex pore structures and heterogeneity. HPMI results also indicate that beach-bar sandstone samples are dominated by micropores, which increase the complexity of pore throat structures and decrease the permeability of sandstone reservoirs. The original depositional environments and later diagenesis determine the pore structure of sandstones, which significantly helps in maintaining and enhancing oil recovery [1, 62, 63]. The depositional environments include the framework grain compositions, size, sorting, and shape and affect the initial pore space among grains. However, the sandstone samples exhibit similar grain compositions, grain sizes, and sorting coefficient (Table 1), which probably indicate that these sandstones exhibit a slightly different initial porosity. Therefore, diagenetic modifications involving compaction, dissolution, and cementation during the burial process further reshape the pore structure and mainly control the sandstone reservoir quality. The petrographic analysis of samples indicates that compaction has the most negative influence on the reservoir quality (Figure 19). Meanwhile, cementation, particularly the content of carbonate cement, also significantly helps in reducing the reservoir quality of sandstones in certain samples owing to a negative correlation between the plane porosity and carbonate cements (Figure 20(a)). Previous researches have also proved that the distance to the sandstone–mudstone contact normally controls the precipitation of early-stage calcite. However, the carbonate in this research mostly consists of late-stage Fe-calcite and ankerite, which is a product of the water–rock reaction and records the signature of diagenetic fluids. The content of carbonate cementation has a negative relationship with the distance to sandstone–mudstone contact, as well as a slightly negative relationship with porosity and permeability (Figures 20(b) and 21), implying mass balance in a closed system within sandstone reservoirs.Figure 19
Diagram showing the compaction porosity loss versus cementation porosity loss in the sandstone reservoirs [65].Figure 20
Relationship between the content of carbonate cement, plane porosity of thin section, and the distance from sandstone–mudstone contact.
(a)(b)Figure 21
Vertical distribution of plane porosity and carbonate content of thin sections, porosity, and permeability in the F1 well in the Boxing Sag. Point A: all intergranular pores are destroyed by strong carbonate cementation; point B: a small amount of intergranular pores and carbonate cements; point C: intergranular pores are relatively common.


## 6. Conclusions

(1)
The Eocene beach-bar sandstones are dominated by micropores in the Boxing Sag and mainly underwent continuous compaction as well as calcite cementation in the early stage; then, calcite and feldspar dissolution were accompanied by the precipitation of quartz and kaolinite as well as the conversion of clay minerals. Intergranular and intragranular pores were partly destroyed by compaction and cemented by Fe-calcite and ankerite in the late stage. Thus, beach-bar sandstone reservoirs generally experienced alkaline–acid–alkaline conditions(2)
The generation of quartz cementation is mainly related to the dissolution of plagioclase with a high calcium content and early calcite providing the silica and Ca2+ source in a closed system. The conversion of clay minerals during the burial process probably contributes a small amount of silica into pore water(3)
Early-stage calcite with a relatively higher proportion of MnO shows yellow luminescence and dissolution signs. Late-stage Fe-calcite and ankerite cements have higher Th than quartz overgrowth and mainly concentrate in Fe2+ and Mg2+ as well as a small number of other cations (Na+, K+, and Sr2+). The diagenetic fluids of carbonate cementation are mainly controlled by the adjacent mudstone owing to the similarity of REE pattern. The dissolution of minerals and the conversion of clay minerals supply extra cations for the reprecipitation of late carbonate locally and induce the fluctuation of δEu values(4)
The compaction significantly reduces pore spaces of beach-bar sandstone reservoirs in the Boxing Sag. Additionally, carbonate cements probably further increase the complexity of pore structure and obey the principle of mass balance.



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*Source: 4981422-2022-01-10.xml*