# Diagenesis and Origination of Carbonate Cements in Deeply Buried Sandstones of the Eocene Es3 Member, Raoyang Sag, Bohai Bay Basin, China

Authors: Kaixun Zhang; Xinxin Fang; Ying Xie; Shun Guo; Zhenwang Liu; Lei Wang
Journal: Geofluids
 (2020)

---

## Abstract

Diagenesis is one of the most predominant factors controlling reservoir quality in the deeply buried siliciclastic sandstones of the third member in the Eocene Shahejie Formation (Es3), in the Raoyang Sag, the Bohai Bay Basin. In this study, thin section, cathodoluminescence (CL), scanning electron microscope (SEM), X-ray diffraction (XRD), Raman spectrum, carbon and oxygen isotopes, and fluid inclusion analyses are used to restructure paragenetic sequences and detect origins of carbonate cements recorded in this deeply buried member. Based on petrographic analyses, the Es3 sandstones are identified as lithic arkoses and feldspathic litharenites at present, but derived from original arkoses and lithic arkoses, respectively. Geohistorically, the Es3 sandstones have undergone two diagenetic episodes of eogenesis and mesogenesis. Events observed during eogenesis include chemical compaction, leaching of feldspar, development of chlorite coating and kaolinite, precipitation of the first generation of quartz overgrowth (QogI), dissolution of feldspar, and precipitation of calcite and nonferroan dolomite cement. Mesogenetic alterations include chemical compaction, precipitation of kaolinite aggregate and the second generation of quartz overgrowth (QogII), precipitation of ankerite, development of I/S and illite, and formation of pyrite. Carbon and oxygen isotopic data show that calcite cements are characterized by 13C (δ13CPDB ranging from -0.7‰ to 1.0‰ with an average of 0.1‰) and 18O (δ18OSMOW varying from 12.3‰ to 19.0‰ with an average of 16.2‰); these stable isotopic data combined with Z value (from 114.69 to 122.18) indicate skeletal debris (δ13CPDB ranging from -1.2‰ to -1.1‰ with an average of -1.15‰; δ18OSMOW varying from 23.0‰ to 23.2‰ with an average of 23.1‰) and ooids in adjacent carbonate beds involved in meteoric water and seawater from outside jointly served as the carbon sources. For nonferroan dolomite, the δ13CPDB value of -4.1‰ is a little bit negative than the calcite, and the δ18OSMOW of 14.3‰ is coincident with the calcite, which suggest the nonferroan dolomites come from the diagenetic fluids with a similar oxygen isotopic composition to that of the calcite but modified by the external acidic δ13C-depleted water. However, the ankerites are actually rich in 12C (δ13CPDB ranging from -10.0‰ to -1.2‰, mean=−4.3‰) and 16O (δ18OSMOW varying from 10.1‰ to 19.4‰, mean=14.9‰), when combined with the distribution of cutting down along the direction pointing to sand-body center from the margin and microthermometric temperature (Th’s) data mainly varying between 115.2°C and 135.5°C with an average of 96.0°C, indicating the main origination from the Es3 source rocks with effective feldspar buffer action for the acidic fluids in the margins of the Es3 sandstones. In addition, the necessary elements for ankerite such as Fe2+, Ca2+, and Mg2+ ions also come from organic matter and clay minerals during thermal maturation of the Es3 source rocks. The study provides insights into diagenetic processes and origination of carbonate cements in the Es3 sandstones; it will facilitate the cognition of predictive models of deeply buried sandstone reservoirs to some extent, which can reduce the risks involved in oil and gas exploration and development.


---

## Body

## 1. Introduction

As hydrocarbon exploration and development expand into technically difficult areas, deeply buried reservoirs have become even more important in recent years [1]. Under these circumstances, diagenesis, especially of deeply buried sandstones, is increasingly considered by geologists as one of the most essential factors controlling the quality of oil and gas reservoir through destroying, enhancing, or preserving porosity and permeability by means of various diagenetic mechanisms [2–9]. Indeed, the study of diagenetic processes based on identifying diagenetic events and paragenetic sequences, which is essential for the understanding and prediction of reservoir quality, not only contributes to enhancing the efficiency of hydrocarbon exploration but also promotes the yields of commercial development [5, 8, 10–13]. Reservoir quality is dependent on both the original depositional environment and postdepositional diagenetic modifications, including physical, chemical, and biological processes, which vary with the pressure, temperature, chemistry of fluids, and framework grains related to the evolution history of sedimentary basin [8, 13–17]. For those deeply buried sandstone reservoirs undergoing complex postdepositional alterations, prediction of reservoir quality faced many more difficulties due to the intricate component transformations that are controlled by fluid-rock interaction [5, 18–22]. As deeply buried sandstones rich in more reactive grains have higher susceptibility to mechanical compaction and more potential cements, dating authigenic mineral is relatively easier to understand the processes and patterns of diagenetic events when combining with compacted features [23].The third member of the Eocene Shahejie Formation (Es3) at a deep burial depth (>3000 m) is one of the most important sandstone reservoirs in the Raoyang Sag, the Bohai Bay Basin. It is mainly made up of deltaic sandstones interbedded with mudstone and lacustrine carbonate rocks, being subjected to a high diagenetic degree. This is the reason why the Es3 reservoir displays remarkable heterogeneity with porosity ranging from 3% to 25% and permeability ranging from 0.01 mD to 100 mD [24–26]. Previous studies from the literatures regarding the Shahejie Formation in Raoyang Sag showed that significant progress has been made in recent years for the successful application of sequence stratigraphy [25, 27, 28]. However, diagenetic evolution of the Es3 sandstones and origins of carbonate cementations have not yet been clearly identified. There have been no systematic studies into the internal connection between the diagenetic alterations and reservoirs quality of the Es3 sandstones as a whole. Nevertheless, various types of diagenetic textures and authigenic minerals are obviously present in these sandstone reservoirs, which provide a large amount of information to reveal the spatial and temporal distribution of diagenesis, and enable paragenetic sequences to be assessed [22, 25, 29, 30].In order to acquire an in-depth and detailed understanding for the key controlling factors of diagenesis and the origins of carbonate cements during and after deposition, a comprehensive, multitechnique approach of quantitative petrographic, mineralogy, fluid inclusion, Raman spectrum, and stable isotope analysis was used. This paper specifically seeks to address the following objectives:(1) To better identify petrological characteristics and diagenetic types of the Es3 member in Raoyang Sag, Bohai Bay Basin(2) To reconstruct the paragenetic sequence of multiple diagenetic events in order to learn the diagenetic history(3) To investigate the originations of the carbonate cements abundant in the Es3 sandstones


## 2. Geological Setting

The Bohai Bay Basin, located in the east of China, is one of the most prolific petroliferous basins, covering a region of approximate 210,000 km2 [29, 31, 32]. Structurally, it is bounded by the Jiaodong uplift to the east, the Taihang Mountains to the west, the Luxi uplift to the south, and the Yanshan Mountains and fold belt to the north [29, 33]. This basin, which formed on the North China platform from the early Tertiary to the Late Jurassic epoch, is a Cenozoic rift lacustrine basin, including six depressions as follows: Linqing, Jiyang, Bozhong, Jizhong, Huanghua, and Liaohe [27, 29, 31] (Figure 1). The tectonic evolution of the basin experienced two major stages, the syn-rift stage from 65.0 Ma to 24.6 Ma, represented by a phase of extensional faulting, and the postrift stage from 24.6 Ma to the present day, represented by the stage of thermal subsidence modified by synchronous strike-slip deformation [29, 34–37]. The syn-rift sequences are composed of Kongdian (Ek), Shahejie, and Dongying (Ed) Formations, deposited in deltaic and lacustrine environments [33, 34, 38, 39]. The postrift sequences consist of the Neogene Guantao (Ng), Minghuazhen (Nm), and the Quaternary Pingyuan (Qp) Formations, which were mainly deposited in fluvial and shallow water delta environments [33, 39–41].Figure 1
Tectonic setting of the Bohai Bay Basin, eastern China, and location map of the Raoyang Sag with its main structural features (modified from [29]).The Raoyang Sag is an interior tectonic unit, which is characterized by a series of normal faults, lying in the central and south Jizhong depression (Figure1). It is a half-graben with several major boundary faults on the northeast side and stratigraphic onlaps toward the southwest slope [42–44]. The Eocene Shahejie Formation comprising the main source rocks, seal rocks and reservoir rocks, is divided into four members from top downwards which are named Es1, Es2, Es3, and Es4 (Figure 2) [25, 27, 31, 45]. Our interval of interest, the Es3 member, is characterized by braid delta facies deposited in shallow to semideep lake environment [24, 27]. Braid channels, subaqueous distributary channels, and channel bays are the predominant microfacies [24, 25]. As a response, large-scale gray sandstones and siltstones intercalated with gray-green and purplish-red mudstones prevailed within Raoyang area [24, 28, 45]. The paleo-climate oscillated frequently between dry and wet in an overall arid to semiarid climatic setting during the depositional period of the Es3 member, with a relative lake level slowly rising due to rapid subsidence of the basement [29].Figure 2
Regional composite lithostratigraphic column of the Raoyang Sag, with average thickness of the various stratigraphic units (modified from [25]).


## 3. Samples and Methods

A total of 112 core samples representative of the Es3 sandstones were collected from 28 bore holes at the depths ranging from 3100 m to 4800 m. All samples were impregnated with blue epoxy and stained with Alizarin Red S to help highlight pore textures and different types of carbonate minerals [46].Petrographic examination was performed on all thin sections for each sample under a Nikon Eclipse E600POL microscope, and at least 300 points per thin section were counted for modal analysis. In addition, replaced and dissolved original components can be identified by optical characteristics of residue, residual shape, residual texture, etc. Cathodoluminescence (CL) was implemented on 35 uncovered thin sections by using a Leica DM2500 P cold cathodoluminoscope under standard operating conditions (16 kV accelerating voltage and 600 mA gun current).In order to test the precipitation temperatures of cements, 25 doubly polished thin sections for microthermometric measurement were selected. Microthermometry was carried out by means of an Olympus BX-60 petrographic microscope equipped with a Linkam THMSG 600 heating and cooling stage. In addition, laser Raman spectrography was performed with a LabRAM HR800. Scanning electron microscope (SEM) at an acceleration voltage of 20 kV was carried out on 45 gold-coated samples to identify 3D textural relationships, especially clay minerals. Similarly, 45 samples were examined by X-ray diffraction (XRD) analyses of separated clay-sized particle fraction for identification of detrital components, cements, and various clay minerals.Based on the identification of ankerite, calcite, and nonferroan dolomite by thin section observation, stable carbon and oxygen isotope testing of carbonate cements were performed on 22 samples. Sufficient powdered microsamples were treated with 100% H3PO4 at 50°C for 48 hours by using a MAT 251 isotope ratio mass spectrometer. The testing conditions and steps can refer to the literature by Swart et al. [47].


## 4. Results

### 4.1. Sandstone Texture and Compositions

According to thin section and SEM observations, the Es3 reservoirs consist of fine to medium grained sandstones, with a grain size from 0.04 to 0.33 mm, but predominantly medium grained sandstones (Figures 3(a) and 3(b)). Under microscope, most of the detrital grains exhibit poorly to moderately sorted, subangular to subrounded shapes (Figure 3(a)), presenting long and concave-convex contacts between different grains (Figure 3(b)). Generally, most of the samples are characterized by rigid components, except for a few rich in biotite, clay mineral, and soft rock fragment (Table 1). Overall, the Es3 sandstones are mineralogically immature with low to medium textural maturity (Figures 3(a), 3(b), and 3(g)).Figure 3
Lithological characteristics of the deeply buried Es3 sandstones in Raoyang Sag. (a) Well NG7: 4077.3 m, fine to medium grained size with poor to moderate sorting, and subangular to subrounded grain shapes, XPL (crosspolarized light). (b) Well L101: 3705.8 m, rigid grains presenting long and concave-convex contact relations (arrow), XPL. (c) Well L425: 3668.2 m, mica containing ferruginous matters existing in samples, XPL. (d) Well L425: 3668.2 m, monocrystalline quartz containing numerous inclusions and bits of polycrystalline quartz (chert) engulfed by carbonate cementation (arrow), XPL. (e) Well N201: 3775.9 m, intensively dissolved feldspar, PPL (plane-polarized light). (f) Well N70X: 3566.3 m, feldspar dissolved along cleavages, SEM. (g) Well L101: 3796.0 m, andesite fragment rich in feldspar with pilotaxitic texture, XPL. (h) Well Ng7: 4077.3 m, ooids and skeletal debris with intact shapes, PPL. Qtz: quartz; Fld: feldspar; RF: rock fragment; Cc: carbonate cements; Mc: mica; Mqtz: monocrystalline quartz; Pqtz: polycrystalline quartz; Plg: plagioclase; Oo: ooid; Sd: skeletal debris.
(a)(b)(c)(d)(e)(f)(g)(h)Table 1
Modal composition by point counting (%) for 15 samples from the deeply buried Es3 sandstones.
Well no.C22Cs1L101L425L446L496N52N63Ng5Samples no.C22-1C22-6Cs1-4Cs1-6L101-2L101-5L101-7L101-8L101-11L425-3L446-7L496-2N52-1N63-5Ng5-9Depth (m)3855.94183.74297.224546.73619.03633.23644.13760.13786.63519.33593.43720.73536.43550.44756.9S.d.m. faceB.c.S.d.c.S.d.c.B.c.B.c.B.c.B.c.S.d.c.S.d.c.B.c.S.d.c.S.d.c.B.c.B.c.B.c.Detrital grains59.262.556.964.361.663.456.367.059.762.361.355.658.943.953.5Original quartz60.065.063.049.059.061.058.053.057.059.065.050.058.062.059.0Present quartz58.063.062.054.058.060.055.052.062.056.064.049.048.055.058.0Monocrystalline49.556.359.447.349.655.149.749.258.551.260.238.044.548.352.2Polycrystalline8.56.72.66.78.44.95.32.83.54.83.811.03.56.75.8Original feldspar32.025.028.040.032.029.025.035.030.027.029.038.025.026.026.0Present feldspar27.020.023.036.033.028.020.034.026.015.026.039.017.017.012.0Plagioclase19.515.819.329.122.023.817.428.123.710.520.231.512.313.910.0K-feldspar7.54.23.76.911.04.22.65.92.34.55.87.54.73.12.0Original R.f.8.010.09.011.09.010.016.012.013.014.06.012.017.012.015.0Present R.f.15.017.015.010.09.012.025.014.012.029.010.012.035.028.030.0Volcanic9.510.0806.06.010.020.09.08.020.08.09.028.020.020.0Metamorphic3.53.63.03.52.01.23.13.82.26.51.01.74.65.16.8Sedimentary2.03.42.00.51.00.81.91.21.82.51.01.32.42.93.2Mica1.51.01.52.01.51.52.50.53.05.01.50.51.02.51.5Ooid and S.d.1.50.51.00.51.00.55.00.51.02.02.51.53.04.00.5Matrix5.25.53.53.55.05.02.52.53.04.53.05.53.52.55.5Au. minerals22.120.422.818.220.619.621.517.521.815.420.226.824.139.030.2Ankerite8.97.56.06.66.06.87.05.59.55.46.711.97.82.311.3Calcite4.23.92.52.73.93.73.54.55.02.53.55.53.429.26.3N.f. dolomite2.81.52.21.52.52.82.01.52.02.01.52.72.11.52.5Qog I3.23.04.73.23.52.33.52.52.02.53.03.03.02.53.0Qog II1.52.13.21.22.52.01.51.51.01.01.01.02.01.51.5Clay1.01.93.22.51.21.53.51.03.21.53.52.24.71.54.3Pyrite0.50.51.00.51.00.50.50.50.10.51.00.51.10.51.3Porosity10.510.114.311.510.310.012.212.011.510.811.510.19.58.19.3R.f.: rock fragment; S.d.: skeletal debris; Au.: authigenic; N.f.: nonferroan; S.d.m. face: sedimentary face; B.c.: brained channel; S.d.c.: subaqueous distributary channel.Thin section point counting indicates that the framework grains of the Es3 sandstones mainly comprise quartz, feldspar, rock fragment, and mica (Figure 3(c) and Table 1). Detrital quartz characterized by monocrystalline (av. 51.3% with min. 38.0% and max. 60.2%) captured numerous fluid inclusions and solid inclusions (Figure 3(d)), suggesting their origin of plutonic rocks. Polycrystalline quartz (Figure 3(d)) is much less common in content by contrast to the monocrystalline (av. 5.7% with min. 2.6% and max. 11.0%) (Table 1). In some cases, detrital quartz shows pitted and embayment-like margins engulfed strongly by carbonate cements (Figure 3(d), Figures 4(g) and 4(h)). Feldspar (Figures 3(e) and 3(f)) is another primary framework constituent, with plagioclases (av. 19.8%, min. 10.0% and max. 29.1%) quantitatively outnumbering K-feldspars (av. 5.1%, min. 2.0% and max. 11.0%) (Table 1). Microscopic investigation reveals an amount of feldspars are dissolved paralleling to the cleavage planes in parent grains under SEM (Figure 3(f)) and extensive carbonatization in plagioclases (Figures 3(b) and 3(d)). Due to the widespread carbonatization and dissolution, the abundance of original feldspars reduced dramatically (Table 1). Rock fragments in the Es3 sandstones mainly derive from volcanic rocks (Figure 3(g)). So, volcanic rock fragment is much more than sedimentary and metamorphic counterpart in content (Table 1). According to point counting, the total contents of all types of rock fragments vary from 9.0% to 35.0% (av. 18.2%). Ooids and skeletal debris are rare (Figure 3(h)), ranging from 0.5% to 4.0% (av. 1.7%).Figure 4
Diagenetic characteristics of the Es3 sandstones in Raoyang Sag. (a) Well L101: 3644.7 m, a large deal of intergranular calcites acting as orange cathodoluminescence, CL. (b) Well N35: 3758.7 m, microcrystalline aggregates of calcite cements stained to be red, XPL. (c) Well NG4: 4680.0 m, rhombic euhedral nonferroan dolomite filling in intergranular pore, SEM. (d) Well L101: 3804.5 m, coarse-grained ankerites stained purple (red arrow) filling intergranular pores and replacing framework grains, PPL. (e) Well L101: 3804.5 m, late ankerite stained purple (black arrow) replacing early calcite stained red (red arrow), PPL. (f) Well L101: 3804.5 m, ankerite cements replacing original quartz grain completely, XPL. (g) Well L101: 3804.20 m, two generations of quartz overgrowths developed around detrital quartz grain, QogI (red arrow) developed continuously and QogII (yellow arrow) developed discontinuously, and engulfed by ankerite (blue arrow), meaning it is prior to ankerite, XPL. (h, i) Well C47: 3628.5 m, ankerite filling intergranular pores and replacing original quartz grains (yellow arrow), as well as nonferroan dolomite (red arrows) engulfing quartz grains, XPL and PPL. Cal: calcite; Ank: ankerite; Qtz: quartz; Nfd: nonferroan dolomite; QogI: the first generation of quartz overgrowths; QogII: the second generation of quartz overgrowths.
(a)(b)(c)(d)(e)(f)(g)(h)(i)Owing to intensive dissolution (Figure3(e)), replacement (Figure 4(f)), and cementation (Figure 4(a)) during burial, petrographic property has gradually changed with transformation in mineral content (Table 1). The present Es3 sandstones are predominantly lithic arkoses and feldspathic litharenites based on composition point counting (Figure 5(a)). Actually, they, respectively, originated from arkose and lithic arkose when trace back to depositional time (Figure 5(b)) by the mean of distinguishing replaced and dissolved original minerals.Figure 5
Present (a) and original (b) detrital compositions of the deeply buried Es3 sandstones.
(a)(b)


### 4.2. Diagenetic Minerals

#### 4.2.1. Carbonate Cements

Carbonate cements are the most predominant authigenic minerals in the Es3 sandstones (Figure 4(a)). Three types including ankerite, calcite, and dolomite were identified by using stained thin sections, CL, and X-ray analyses. Point counting data show ankerite abundance is much higher than the other carbonate cements, varying from 2.3% to 11.9% (av. 7.3%) (Table 1). These ankerites occur in the form of poikilotopic patches (Figures 4(a) and 4(d)) filling pore spaces and engulfing the margins of framework grains (Figure 4(d)) or early carbonate cements (Figure 4(e)). In some cases, detrital grains were replaced completely by these overgrown ankerites, so that those original components changed thoroughly as a result (Figure 4(f)). Calcite is subordinate to ankerite in content and ranges from 2.5% to 29.2% (av. 5.6%) (Table 1). Generally, it occurs as microcrystalline aggregate filling in intergranular pores, which was stained dark red color in stained thin sections (Figure 4(b)). Rhombic nonferroan dolomite under SEM is rare (Table 1) and presents as scattered cements occluding primary pores or engulfing detrital grains (Figures 4(h) and 4(i)).


#### 4.2.2. Quartz Cements

Authigenic quartz cements are mostly observed as syntaxial euhedral macrocrystalline overgrowths with a thickness from 5.0 to 62.0μm around the detrital quartz grains in thin sections (Figure 4(g)), while prismatic outgrowths can easily be observed morphologically under SEM. Generally, linear fluid inclusion cluster and/or clay coatings near the grain margins are the signs for overgrowth and generation discrimination. There are two identified generations of the quartz overgrowths (Figure 4(g)). According to point counting, the first generation (QogI) is comparatively far more widespread (2.0% to 4.7% with an average of 3.0%) than those of the second generation (QogII) in coincidence with the content ranging from 1.0% to 3.2% with an average of 1.6% (Table 1). Thin sections show that QogI prefers to develop continuously at the places where clay coatings are rare (Figure 4(g)). However, QogII usually developed discontinuously and intermittently.


#### 4.2.3. Authigenic Clays

According to SEM morphologic characteristics combined with mineralogic analysis, there are four types of authigenic clay minerals (i.e., mix-layered illite/smectite, kaolinite, chlorite, and illite) developed in the Es3 sandstones (Table 2 and Figure 6). Mix-layered illite/smectite (I/S), as an intermediate transformable product of smectite into illite, mainly takes the forms of foliage and/or honeycomb (Figure 7(a)). XRD indicates I/S occupies absolute dominance in total clay minerals with an average content of 62.4% (from 30.2% to 97.4%) (Table 2). Kaolinite is another prevailing mineral and occurs individually as pseudohexagonal euhedral crystal. There are two types of kaolinite developing in the samples according to occurrences, the one attaching to grain surfaces modified by pore fluids (Figure 7(b)) and the other one aggregating as clusters; kaolinite clusters often take the booklet-like or vermicular-stacked aggregate forms occluding pores near detrital feldspars (Figure 7(c)). Chlorite is also abundant in volume and its importance ought not be neglected. Generally, it develops in the form of rose-like sheaf, displays microcrystalline habits, and covers on the grain surfaces acting as chlorite coatings (Figures 7(d) and 7(e)). Authigenic illite polytypes often occur as pore-bridging cements consisting of fibrous crystals with long axis perpendicular to grain surfaces. Fibrous illites often grow into pores and block pore throats resulting in a drastic reduction in permeability (Figure 7(f)).Table 2
X-ray diffraction of clay fractions in Es3 member sandstones.
WellDepth (m)Sample no.KaoliniteChloriteSmectiteIlliteMix-layered illite-smectiteC473627.4Ch47-227.230.3/4.038.5N70x3565.9N70x-849.116.5/4.230.2Ng74078.0Ng7-6/12.5/4.083.5L1013719.8L101-5/44.3/5.550.2L1013643.6L101-629.031.0/8.032.0L1013679.7L101-9///2.697.4N1013775.9N101-712.3//12.276.5N353758.7N35-211.1//6.382.6N2013547.8N201-714.311.1/8.366.3L1073850.5L107-312.214.4/6.566.9Figure 6
Representative clay fraction XRD spectra of the Es3 sandstone reservoirs in Raoyang Sag. Kao: kaolinite; Ilt: illite; I/S: illite/smectite; Chl: chlorite.Figure 7
Diagenetic characteristics of the deeply buried Es3 sandstones in Raoyang Sag. (a) Well LG3: 3824.3 m, I/S taking place as the forms of foliage and/or honeycomb, SEM. (b) Well L425: 3662.6 m, modified kaolinite to some extent attaching to grain surfaces, SEM. (c) Well N62: 3565.5 m, kaolinite aggregates developing in pores near dissolved feldspars, SEM. (d, e) Well N35: 3758.7 m, chlorite coating growing around framework grains, PPL and SEM. (f) Well L101: 3804.2 m, illite acting as fibrous crystals with long axis perpendicular to grain surfaces, XPL. (g, h) Well N35: 3758.72 m, pyrite engulfing and replacing quartz, feldspar, and ankerite, XPL and RL. I/S: illite/smectite; Kao: kaolinite; Plg: plagioclase; Fld: feldspar; Chl: chlorite; Py: pyrite; Qtz: quartz; Ilt: illite; RL: reflected light.
(a)(b)(c)(d)(e)(f)(g)(h)


#### 4.2.4. Pyrite

Pyrite is traced in amount and distributes in examined samples as subregular patches (Figures7(g) and 7(h)). It is easy to be identified in intergranular pores because of its characteristic for opaqueness to light. In thin sections, pyrite engulfs and thus postdates ankerite cements, implying its formation time of mesogenetic period.


### 4.3. Fluid Inclusion Analysis

Poikilotopic ankerite cements host a large deal of two-phase aqueous-dominated primary fluid inclusions with tiny gas bubbles (Figure8). In addition, those inclusions are large enough with a size ranging from 2 to 16 μm for homogenization temperature (Th’s) measurements. Microthermometric data shows that the ankerite cement Th’s have an average of 96.0°C mainly varying between 115.2°C and 135.5°C (Figure 9).Figure 8
Photomicrograph of two-phase fluid inclusions in ankerite cement from the Es3 sandstones under crosspolarized light (a) and fluorescent light (b).
(a)(b)Figure 9
Histogram of homogenization temperatures (Th) from all primary fluid inclusions from the late ankerite cements in the Es3 sandstones (n=57).


### 4.4. Carbon and Oxygen Isotopic Composition

The data of carbon and oxygen isotope analysis on ankerite, calcite, and nonferroan dolomite cements are shown in Table3 and Figure 10. For ankerite cement, δ13CPDB value varies between -10.0‰ and -1.2‰ with an average of -4.3‰ and δ18OSMOW value varies between 10.1‰ and 19.4‰ with average of 14.9‰. For calcite cement, δ13CPDB value ranges from -0.7‰ to 1.0‰ with an average of -0.1‰ and δ18OSMOW value ranges from 12.3‰ to 19.0‰ with average of 16.2‰. For nonferroan dolomite cement, δ13CPDB value is -4.1‰, and δ18OSMOW value is 14.3‰. For skeletal debris, δ13CPDB value varies between -1.2‰ and -1.1‰ with an average of -1.15‰ and δ18OSMOW value varies between 23.0‰ and 23.2‰ with average of 23.1‰.Table 3
Mineralogical and isotopic composition of carbonate cements, and calculated formation temperature of cements in the Es3 sandstone reservoirs.
WellsDepth (m)Mineral typesOccurrenceTimeδ13CPDB (‰)δ18OPDB (‰)δ18OSMOW (‰)Z valueC473627.40CalciteMicrocrystallineEarly1.0-14.516.0122.18CS14293.68CalciteMicrocrystallineEarly0.1-13.017.5121.02CS14540.81AnkeritePoikilotopicLate-1.2-14.216.3117.74L1013811.54AnkeritePoikilotopicEarly-4.9-17.912.5108.57L1013782.26AnkeriteMacrocrystallineLate-5.0-17.213.2108.51L1013757.18AnkeriteMacrocrystallineLate-5.4-17.413.0107.58L1013633.18N.f. dolomiteMacrocrystallineMedium-4.1-16.114.3110.87L4253693.75AnkeritePoikilotopicLate-5.2-15.614.8108.85L4253541.75AnkeritePoikilotopicLate-5.2-15.615.9108.85L4253599.10CalcitePoikilotopicEarly-0.7-18.112.3116.78NG54756.88CalcitePoikilotopicEarly-0.6-11.519.0120.22LG24250.34AnkeriteMacrocrystallineLate-5.9-17.812.0106.26C224117.46AnkeriteMacrocrystallineLate-3.6-12.717.8113.55N413522.12AnkeriteMacrocrystallineLate-3.7-14.815.6112.27N413507.43AnkeriteMacrocrystallineLate-2.0-12.817.8116.89N2013547.78AnkeriteMacrocrystallineLate-2.5-15.015.4121.16N623565.50CalcitePoikilotopicEarly-0.4-14.316.1114.69N633548.71AnkeritePoikilotopicLate-1.9-11.219.4121.05N70X3566.32AnkeriteMacrocrystallineLate-10.0-15.415.1119.34N523539.30AnkeriteMicrocrystallineLate-3.5-20.210.1117.85N353750.75BioclastsEarly-1.1-7.623.099.21N2013764.36BioclastsEarly-1.2-7.423.2110.09Figure 10
Distribution characteristics of carbon and oxygen isotopes for carbonate cements.


## 4.1. Sandstone Texture and Compositions

According to thin section and SEM observations, the Es3 reservoirs consist of fine to medium grained sandstones, with a grain size from 0.04 to 0.33 mm, but predominantly medium grained sandstones (Figures 3(a) and 3(b)). Under microscope, most of the detrital grains exhibit poorly to moderately sorted, subangular to subrounded shapes (Figure 3(a)), presenting long and concave-convex contacts between different grains (Figure 3(b)). Generally, most of the samples are characterized by rigid components, except for a few rich in biotite, clay mineral, and soft rock fragment (Table 1). Overall, the Es3 sandstones are mineralogically immature with low to medium textural maturity (Figures 3(a), 3(b), and 3(g)).Figure 3
Lithological characteristics of the deeply buried Es3 sandstones in Raoyang Sag. (a) Well NG7: 4077.3 m, fine to medium grained size with poor to moderate sorting, and subangular to subrounded grain shapes, XPL (crosspolarized light). (b) Well L101: 3705.8 m, rigid grains presenting long and concave-convex contact relations (arrow), XPL. (c) Well L425: 3668.2 m, mica containing ferruginous matters existing in samples, XPL. (d) Well L425: 3668.2 m, monocrystalline quartz containing numerous inclusions and bits of polycrystalline quartz (chert) engulfed by carbonate cementation (arrow), XPL. (e) Well N201: 3775.9 m, intensively dissolved feldspar, PPL (plane-polarized light). (f) Well N70X: 3566.3 m, feldspar dissolved along cleavages, SEM. (g) Well L101: 3796.0 m, andesite fragment rich in feldspar with pilotaxitic texture, XPL. (h) Well Ng7: 4077.3 m, ooids and skeletal debris with intact shapes, PPL. Qtz: quartz; Fld: feldspar; RF: rock fragment; Cc: carbonate cements; Mc: mica; Mqtz: monocrystalline quartz; Pqtz: polycrystalline quartz; Plg: plagioclase; Oo: ooid; Sd: skeletal debris.
(a)(b)(c)(d)(e)(f)(g)(h)Table 1
Modal composition by point counting (%) for 15 samples from the deeply buried Es3 sandstones.
Well no.C22Cs1L101L425L446L496N52N63Ng5Samples no.C22-1C22-6Cs1-4Cs1-6L101-2L101-5L101-7L101-8L101-11L425-3L446-7L496-2N52-1N63-5Ng5-9Depth (m)3855.94183.74297.224546.73619.03633.23644.13760.13786.63519.33593.43720.73536.43550.44756.9S.d.m. faceB.c.S.d.c.S.d.c.B.c.B.c.B.c.B.c.S.d.c.S.d.c.B.c.S.d.c.S.d.c.B.c.B.c.B.c.Detrital grains59.262.556.964.361.663.456.367.059.762.361.355.658.943.953.5Original quartz60.065.063.049.059.061.058.053.057.059.065.050.058.062.059.0Present quartz58.063.062.054.058.060.055.052.062.056.064.049.048.055.058.0Monocrystalline49.556.359.447.349.655.149.749.258.551.260.238.044.548.352.2Polycrystalline8.56.72.66.78.44.95.32.83.54.83.811.03.56.75.8Original feldspar32.025.028.040.032.029.025.035.030.027.029.038.025.026.026.0Present feldspar27.020.023.036.033.028.020.034.026.015.026.039.017.017.012.0Plagioclase19.515.819.329.122.023.817.428.123.710.520.231.512.313.910.0K-feldspar7.54.23.76.911.04.22.65.92.34.55.87.54.73.12.0Original R.f.8.010.09.011.09.010.016.012.013.014.06.012.017.012.015.0Present R.f.15.017.015.010.09.012.025.014.012.029.010.012.035.028.030.0Volcanic9.510.0806.06.010.020.09.08.020.08.09.028.020.020.0Metamorphic3.53.63.03.52.01.23.13.82.26.51.01.74.65.16.8Sedimentary2.03.42.00.51.00.81.91.21.82.51.01.32.42.93.2Mica1.51.01.52.01.51.52.50.53.05.01.50.51.02.51.5Ooid and S.d.1.50.51.00.51.00.55.00.51.02.02.51.53.04.00.5Matrix5.25.53.53.55.05.02.52.53.04.53.05.53.52.55.5Au. minerals22.120.422.818.220.619.621.517.521.815.420.226.824.139.030.2Ankerite8.97.56.06.66.06.87.05.59.55.46.711.97.82.311.3Calcite4.23.92.52.73.93.73.54.55.02.53.55.53.429.26.3N.f. dolomite2.81.52.21.52.52.82.01.52.02.01.52.72.11.52.5Qog I3.23.04.73.23.52.33.52.52.02.53.03.03.02.53.0Qog II1.52.13.21.22.52.01.51.51.01.01.01.02.01.51.5Clay1.01.93.22.51.21.53.51.03.21.53.52.24.71.54.3Pyrite0.50.51.00.51.00.50.50.50.10.51.00.51.10.51.3Porosity10.510.114.311.510.310.012.212.011.510.811.510.19.58.19.3R.f.: rock fragment; S.d.: skeletal debris; Au.: authigenic; N.f.: nonferroan; S.d.m. face: sedimentary face; B.c.: brained channel; S.d.c.: subaqueous distributary channel.Thin section point counting indicates that the framework grains of the Es3 sandstones mainly comprise quartz, feldspar, rock fragment, and mica (Figure 3(c) and Table 1). Detrital quartz characterized by monocrystalline (av. 51.3% with min. 38.0% and max. 60.2%) captured numerous fluid inclusions and solid inclusions (Figure 3(d)), suggesting their origin of plutonic rocks. Polycrystalline quartz (Figure 3(d)) is much less common in content by contrast to the monocrystalline (av. 5.7% with min. 2.6% and max. 11.0%) (Table 1). In some cases, detrital quartz shows pitted and embayment-like margins engulfed strongly by carbonate cements (Figure 3(d), Figures 4(g) and 4(h)). Feldspar (Figures 3(e) and 3(f)) is another primary framework constituent, with plagioclases (av. 19.8%, min. 10.0% and max. 29.1%) quantitatively outnumbering K-feldspars (av. 5.1%, min. 2.0% and max. 11.0%) (Table 1). Microscopic investigation reveals an amount of feldspars are dissolved paralleling to the cleavage planes in parent grains under SEM (Figure 3(f)) and extensive carbonatization in plagioclases (Figures 3(b) and 3(d)). Due to the widespread carbonatization and dissolution, the abundance of original feldspars reduced dramatically (Table 1). Rock fragments in the Es3 sandstones mainly derive from volcanic rocks (Figure 3(g)). So, volcanic rock fragment is much more than sedimentary and metamorphic counterpart in content (Table 1). According to point counting, the total contents of all types of rock fragments vary from 9.0% to 35.0% (av. 18.2%). Ooids and skeletal debris are rare (Figure 3(h)), ranging from 0.5% to 4.0% (av. 1.7%).Figure 4
Diagenetic characteristics of the Es3 sandstones in Raoyang Sag. (a) Well L101: 3644.7 m, a large deal of intergranular calcites acting as orange cathodoluminescence, CL. (b) Well N35: 3758.7 m, microcrystalline aggregates of calcite cements stained to be red, XPL. (c) Well NG4: 4680.0 m, rhombic euhedral nonferroan dolomite filling in intergranular pore, SEM. (d) Well L101: 3804.5 m, coarse-grained ankerites stained purple (red arrow) filling intergranular pores and replacing framework grains, PPL. (e) Well L101: 3804.5 m, late ankerite stained purple (black arrow) replacing early calcite stained red (red arrow), PPL. (f) Well L101: 3804.5 m, ankerite cements replacing original quartz grain completely, XPL. (g) Well L101: 3804.20 m, two generations of quartz overgrowths developed around detrital quartz grain, QogI (red arrow) developed continuously and QogII (yellow arrow) developed discontinuously, and engulfed by ankerite (blue arrow), meaning it is prior to ankerite, XPL. (h, i) Well C47: 3628.5 m, ankerite filling intergranular pores and replacing original quartz grains (yellow arrow), as well as nonferroan dolomite (red arrows) engulfing quartz grains, XPL and PPL. Cal: calcite; Ank: ankerite; Qtz: quartz; Nfd: nonferroan dolomite; QogI: the first generation of quartz overgrowths; QogII: the second generation of quartz overgrowths.
(a)(b)(c)(d)(e)(f)(g)(h)(i)Owing to intensive dissolution (Figure3(e)), replacement (Figure 4(f)), and cementation (Figure 4(a)) during burial, petrographic property has gradually changed with transformation in mineral content (Table 1). The present Es3 sandstones are predominantly lithic arkoses and feldspathic litharenites based on composition point counting (Figure 5(a)). Actually, they, respectively, originated from arkose and lithic arkose when trace back to depositional time (Figure 5(b)) by the mean of distinguishing replaced and dissolved original minerals.Figure 5
Present (a) and original (b) detrital compositions of the deeply buried Es3 sandstones.
(a)(b)


## 4.2. Diagenetic Minerals

### 4.2.1. Carbonate Cements

Carbonate cements are the most predominant authigenic minerals in the Es3 sandstones (Figure 4(a)). Three types including ankerite, calcite, and dolomite were identified by using stained thin sections, CL, and X-ray analyses. Point counting data show ankerite abundance is much higher than the other carbonate cements, varying from 2.3% to 11.9% (av. 7.3%) (Table 1). These ankerites occur in the form of poikilotopic patches (Figures 4(a) and 4(d)) filling pore spaces and engulfing the margins of framework grains (Figure 4(d)) or early carbonate cements (Figure 4(e)). In some cases, detrital grains were replaced completely by these overgrown ankerites, so that those original components changed thoroughly as a result (Figure 4(f)). Calcite is subordinate to ankerite in content and ranges from 2.5% to 29.2% (av. 5.6%) (Table 1). Generally, it occurs as microcrystalline aggregate filling in intergranular pores, which was stained dark red color in stained thin sections (Figure 4(b)). Rhombic nonferroan dolomite under SEM is rare (Table 1) and presents as scattered cements occluding primary pores or engulfing detrital grains (Figures 4(h) and 4(i)).


### 4.2.2. Quartz Cements

Authigenic quartz cements are mostly observed as syntaxial euhedral macrocrystalline overgrowths with a thickness from 5.0 to 62.0μm around the detrital quartz grains in thin sections (Figure 4(g)), while prismatic outgrowths can easily be observed morphologically under SEM. Generally, linear fluid inclusion cluster and/or clay coatings near the grain margins are the signs for overgrowth and generation discrimination. There are two identified generations of the quartz overgrowths (Figure 4(g)). According to point counting, the first generation (QogI) is comparatively far more widespread (2.0% to 4.7% with an average of 3.0%) than those of the second generation (QogII) in coincidence with the content ranging from 1.0% to 3.2% with an average of 1.6% (Table 1). Thin sections show that QogI prefers to develop continuously at the places where clay coatings are rare (Figure 4(g)). However, QogII usually developed discontinuously and intermittently.


### 4.2.3. Authigenic Clays

According to SEM morphologic characteristics combined with mineralogic analysis, there are four types of authigenic clay minerals (i.e., mix-layered illite/smectite, kaolinite, chlorite, and illite) developed in the Es3 sandstones (Table 2 and Figure 6). Mix-layered illite/smectite (I/S), as an intermediate transformable product of smectite into illite, mainly takes the forms of foliage and/or honeycomb (Figure 7(a)). XRD indicates I/S occupies absolute dominance in total clay minerals with an average content of 62.4% (from 30.2% to 97.4%) (Table 2). Kaolinite is another prevailing mineral and occurs individually as pseudohexagonal euhedral crystal. There are two types of kaolinite developing in the samples according to occurrences, the one attaching to grain surfaces modified by pore fluids (Figure 7(b)) and the other one aggregating as clusters; kaolinite clusters often take the booklet-like or vermicular-stacked aggregate forms occluding pores near detrital feldspars (Figure 7(c)). Chlorite is also abundant in volume and its importance ought not be neglected. Generally, it develops in the form of rose-like sheaf, displays microcrystalline habits, and covers on the grain surfaces acting as chlorite coatings (Figures 7(d) and 7(e)). Authigenic illite polytypes often occur as pore-bridging cements consisting of fibrous crystals with long axis perpendicular to grain surfaces. Fibrous illites often grow into pores and block pore throats resulting in a drastic reduction in permeability (Figure 7(f)).Table 2
X-ray diffraction of clay fractions in Es3 member sandstones.
WellDepth (m)Sample no.KaoliniteChloriteSmectiteIlliteMix-layered illite-smectiteC473627.4Ch47-227.230.3/4.038.5N70x3565.9N70x-849.116.5/4.230.2Ng74078.0Ng7-6/12.5/4.083.5L1013719.8L101-5/44.3/5.550.2L1013643.6L101-629.031.0/8.032.0L1013679.7L101-9///2.697.4N1013775.9N101-712.3//12.276.5N353758.7N35-211.1//6.382.6N2013547.8N201-714.311.1/8.366.3L1073850.5L107-312.214.4/6.566.9Figure 6
Representative clay fraction XRD spectra of the Es3 sandstone reservoirs in Raoyang Sag. Kao: kaolinite; Ilt: illite; I/S: illite/smectite; Chl: chlorite.Figure 7
Diagenetic characteristics of the deeply buried Es3 sandstones in Raoyang Sag. (a) Well LG3: 3824.3 m, I/S taking place as the forms of foliage and/or honeycomb, SEM. (b) Well L425: 3662.6 m, modified kaolinite to some extent attaching to grain surfaces, SEM. (c) Well N62: 3565.5 m, kaolinite aggregates developing in pores near dissolved feldspars, SEM. (d, e) Well N35: 3758.7 m, chlorite coating growing around framework grains, PPL and SEM. (f) Well L101: 3804.2 m, illite acting as fibrous crystals with long axis perpendicular to grain surfaces, XPL. (g, h) Well N35: 3758.72 m, pyrite engulfing and replacing quartz, feldspar, and ankerite, XPL and RL. I/S: illite/smectite; Kao: kaolinite; Plg: plagioclase; Fld: feldspar; Chl: chlorite; Py: pyrite; Qtz: quartz; Ilt: illite; RL: reflected light.
(a)(b)(c)(d)(e)(f)(g)(h)


### 4.2.4. Pyrite

Pyrite is traced in amount and distributes in examined samples as subregular patches (Figures7(g) and 7(h)). It is easy to be identified in intergranular pores because of its characteristic for opaqueness to light. In thin sections, pyrite engulfs and thus postdates ankerite cements, implying its formation time of mesogenetic period.


## 4.2.1. Carbonate Cements

Carbonate cements are the most predominant authigenic minerals in the Es3 sandstones (Figure 4(a)). Three types including ankerite, calcite, and dolomite were identified by using stained thin sections, CL, and X-ray analyses. Point counting data show ankerite abundance is much higher than the other carbonate cements, varying from 2.3% to 11.9% (av. 7.3%) (Table 1). These ankerites occur in the form of poikilotopic patches (Figures 4(a) and 4(d)) filling pore spaces and engulfing the margins of framework grains (Figure 4(d)) or early carbonate cements (Figure 4(e)). In some cases, detrital grains were replaced completely by these overgrown ankerites, so that those original components changed thoroughly as a result (Figure 4(f)). Calcite is subordinate to ankerite in content and ranges from 2.5% to 29.2% (av. 5.6%) (Table 1). Generally, it occurs as microcrystalline aggregate filling in intergranular pores, which was stained dark red color in stained thin sections (Figure 4(b)). Rhombic nonferroan dolomite under SEM is rare (Table 1) and presents as scattered cements occluding primary pores or engulfing detrital grains (Figures 4(h) and 4(i)).


## 4.2.2. Quartz Cements

Authigenic quartz cements are mostly observed as syntaxial euhedral macrocrystalline overgrowths with a thickness from 5.0 to 62.0μm around the detrital quartz grains in thin sections (Figure 4(g)), while prismatic outgrowths can easily be observed morphologically under SEM. Generally, linear fluid inclusion cluster and/or clay coatings near the grain margins are the signs for overgrowth and generation discrimination. There are two identified generations of the quartz overgrowths (Figure 4(g)). According to point counting, the first generation (QogI) is comparatively far more widespread (2.0% to 4.7% with an average of 3.0%) than those of the second generation (QogII) in coincidence with the content ranging from 1.0% to 3.2% with an average of 1.6% (Table 1). Thin sections show that QogI prefers to develop continuously at the places where clay coatings are rare (Figure 4(g)). However, QogII usually developed discontinuously and intermittently.


## 4.2.3. Authigenic Clays

According to SEM morphologic characteristics combined with mineralogic analysis, there are four types of authigenic clay minerals (i.e., mix-layered illite/smectite, kaolinite, chlorite, and illite) developed in the Es3 sandstones (Table 2 and Figure 6). Mix-layered illite/smectite (I/S), as an intermediate transformable product of smectite into illite, mainly takes the forms of foliage and/or honeycomb (Figure 7(a)). XRD indicates I/S occupies absolute dominance in total clay minerals with an average content of 62.4% (from 30.2% to 97.4%) (Table 2). Kaolinite is another prevailing mineral and occurs individually as pseudohexagonal euhedral crystal. There are two types of kaolinite developing in the samples according to occurrences, the one attaching to grain surfaces modified by pore fluids (Figure 7(b)) and the other one aggregating as clusters; kaolinite clusters often take the booklet-like or vermicular-stacked aggregate forms occluding pores near detrital feldspars (Figure 7(c)). Chlorite is also abundant in volume and its importance ought not be neglected. Generally, it develops in the form of rose-like sheaf, displays microcrystalline habits, and covers on the grain surfaces acting as chlorite coatings (Figures 7(d) and 7(e)). Authigenic illite polytypes often occur as pore-bridging cements consisting of fibrous crystals with long axis perpendicular to grain surfaces. Fibrous illites often grow into pores and block pore throats resulting in a drastic reduction in permeability (Figure 7(f)).Table 2
X-ray diffraction of clay fractions in Es3 member sandstones.
WellDepth (m)Sample no.KaoliniteChloriteSmectiteIlliteMix-layered illite-smectiteC473627.4Ch47-227.230.3/4.038.5N70x3565.9N70x-849.116.5/4.230.2Ng74078.0Ng7-6/12.5/4.083.5L1013719.8L101-5/44.3/5.550.2L1013643.6L101-629.031.0/8.032.0L1013679.7L101-9///2.697.4N1013775.9N101-712.3//12.276.5N353758.7N35-211.1//6.382.6N2013547.8N201-714.311.1/8.366.3L1073850.5L107-312.214.4/6.566.9Figure 6
Representative clay fraction XRD spectra of the Es3 sandstone reservoirs in Raoyang Sag. Kao: kaolinite; Ilt: illite; I/S: illite/smectite; Chl: chlorite.Figure 7
Diagenetic characteristics of the deeply buried Es3 sandstones in Raoyang Sag. (a) Well LG3: 3824.3 m, I/S taking place as the forms of foliage and/or honeycomb, SEM. (b) Well L425: 3662.6 m, modified kaolinite to some extent attaching to grain surfaces, SEM. (c) Well N62: 3565.5 m, kaolinite aggregates developing in pores near dissolved feldspars, SEM. (d, e) Well N35: 3758.7 m, chlorite coating growing around framework grains, PPL and SEM. (f) Well L101: 3804.2 m, illite acting as fibrous crystals with long axis perpendicular to grain surfaces, XPL. (g, h) Well N35: 3758.72 m, pyrite engulfing and replacing quartz, feldspar, and ankerite, XPL and RL. I/S: illite/smectite; Kao: kaolinite; Plg: plagioclase; Fld: feldspar; Chl: chlorite; Py: pyrite; Qtz: quartz; Ilt: illite; RL: reflected light.
(a)(b)(c)(d)(e)(f)(g)(h)


## 4.2.4. Pyrite

Pyrite is traced in amount and distributes in examined samples as subregular patches (Figures7(g) and 7(h)). It is easy to be identified in intergranular pores because of its characteristic for opaqueness to light. In thin sections, pyrite engulfs and thus postdates ankerite cements, implying its formation time of mesogenetic period.


## 4.3. Fluid Inclusion Analysis

Poikilotopic ankerite cements host a large deal of two-phase aqueous-dominated primary fluid inclusions with tiny gas bubbles (Figure8). In addition, those inclusions are large enough with a size ranging from 2 to 16 μm for homogenization temperature (Th’s) measurements. Microthermometric data shows that the ankerite cement Th’s have an average of 96.0°C mainly varying between 115.2°C and 135.5°C (Figure 9).Figure 8
Photomicrograph of two-phase fluid inclusions in ankerite cement from the Es3 sandstones under crosspolarized light (a) and fluorescent light (b).
(a)(b)Figure 9
Histogram of homogenization temperatures (Th) from all primary fluid inclusions from the late ankerite cements in the Es3 sandstones (n=57).


## 4.4. Carbon and Oxygen Isotopic Composition

The data of carbon and oxygen isotope analysis on ankerite, calcite, and nonferroan dolomite cements are shown in Table3 and Figure 10. For ankerite cement, δ13CPDB value varies between -10.0‰ and -1.2‰ with an average of -4.3‰ and δ18OSMOW value varies between 10.1‰ and 19.4‰ with average of 14.9‰. For calcite cement, δ13CPDB value ranges from -0.7‰ to 1.0‰ with an average of -0.1‰ and δ18OSMOW value ranges from 12.3‰ to 19.0‰ with average of 16.2‰. For nonferroan dolomite cement, δ13CPDB value is -4.1‰, and δ18OSMOW value is 14.3‰. For skeletal debris, δ13CPDB value varies between -1.2‰ and -1.1‰ with an average of -1.15‰ and δ18OSMOW value varies between 23.0‰ and 23.2‰ with average of 23.1‰.Table 3
Mineralogical and isotopic composition of carbonate cements, and calculated formation temperature of cements in the Es3 sandstone reservoirs.
WellsDepth (m)Mineral typesOccurrenceTimeδ13CPDB (‰)δ18OPDB (‰)δ18OSMOW (‰)Z valueC473627.40CalciteMicrocrystallineEarly1.0-14.516.0122.18CS14293.68CalciteMicrocrystallineEarly0.1-13.017.5121.02CS14540.81AnkeritePoikilotopicLate-1.2-14.216.3117.74L1013811.54AnkeritePoikilotopicEarly-4.9-17.912.5108.57L1013782.26AnkeriteMacrocrystallineLate-5.0-17.213.2108.51L1013757.18AnkeriteMacrocrystallineLate-5.4-17.413.0107.58L1013633.18N.f. dolomiteMacrocrystallineMedium-4.1-16.114.3110.87L4253693.75AnkeritePoikilotopicLate-5.2-15.614.8108.85L4253541.75AnkeritePoikilotopicLate-5.2-15.615.9108.85L4253599.10CalcitePoikilotopicEarly-0.7-18.112.3116.78NG54756.88CalcitePoikilotopicEarly-0.6-11.519.0120.22LG24250.34AnkeriteMacrocrystallineLate-5.9-17.812.0106.26C224117.46AnkeriteMacrocrystallineLate-3.6-12.717.8113.55N413522.12AnkeriteMacrocrystallineLate-3.7-14.815.6112.27N413507.43AnkeriteMacrocrystallineLate-2.0-12.817.8116.89N2013547.78AnkeriteMacrocrystallineLate-2.5-15.015.4121.16N623565.50CalcitePoikilotopicEarly-0.4-14.316.1114.69N633548.71AnkeritePoikilotopicLate-1.9-11.219.4121.05N70X3566.32AnkeriteMacrocrystallineLate-10.0-15.415.1119.34N523539.30AnkeriteMicrocrystallineLate-3.5-20.210.1117.85N353750.75BioclastsEarly-1.1-7.623.099.21N2013764.36BioclastsEarly-1.2-7.423.2110.09Figure 10
Distribution characteristics of carbon and oxygen isotopes for carbonate cements.


## 5. Discussion

### 5.1. Diagenetic Events and Paragenetic Sequences

Diagenetic processes of the Es3 sandstones have undergone two diagenetic stages: eogenesis (with maximum burial depth of 1.0-2.0 km and maximum temperature of 30-70°C, approximately) and mesogenesis (with burial depth deeper than 1.0-2.0 km and temperature higher than 30-70°C) [6, 13]. Actually, it is impossible to precisely measure absolute time and duration of each diagenetic event in detail. However, paragenetic sequences during burial can be reconstructed approximately by considering the diagenetic environments and mutual textural relations between authigenic components and/or initial constituents [23, 48].


#### 5.1.1. Eogenetic Processes

Prior to becoming sedimentary rocks, all sediments had suffered diagenetic alterations at or near the surface of sediment pile, which is mainly influenced by the intergranular fluids deriving from depositional environment in an open system [6, 49]. First of all, mechanical compaction, which is more effective at packing loose sediments and driving intergranular water expulsion in initial burial stage, took place gradually in response to the increasing vertical stress [5, 6, 50]. Then, these sediments have been subjected to mechanical and chemical weathering alterations soon after deposition in the arid to semiarid climate during Es3 period [26], which would inevitably lead to leaching of feldspar with respect to the flowing formation fluids by involving in infiltrated meteoric water [18, 51]. Petrographic observations show feldspars are often dissolved along cleavage significantly and thus create a mass of secondary pores (Figures 3(e) and 3(f)). At the same time, various authigenic clay minerals were produced, among which chlorite coatings formed firstly attaching to detrital grain surfaces, as there is not any other authigenic mineral existing in the space between the detrital grain and chlorite coating (Figure 7(d)), and mostly chlorite coatings contact directly with those detrital grains (Figure 7(e)). Additionally, these chlorite coatings not only protected original pores by enhancing the ability for resisting compaction but also served as barriers to retard the development of quartz overgrowths [49, 52]. Kaolinite is another important type of early clay mineral growing on the surfaces of detrital grains. Under SEM, these kaolinites had been modified with a low-level of euhedral texture (Figure 7(b)). Although these kaolinites were associated with feldspar leaching, yet they were removed timely and immediately in the flowing solution [30]. So, the random distribution of these kaolinites in samples was developed instead of concentrating in local position near secondary leaching pores [18, 30]. Except for early clay cements, calcite was a nonnegligible scenario in the eogenetic processes (Figure 4(b)). In some cases, those intergranular calcites characterized by fine microcrystal assemblage reach up to 29.2% in volume (Table 1 and Figure 4(a)). This is indicative of its early origin as only during the early stage of the eogenetic period can the sediments provide such spacious intergranular volumes for calcite development. On the other hand, these authigenic calcites directly cover the chlorite coatings or detrital grain surfaces in textural relations and thus postdate the authigenic chlorites (Figure 4(b)). In addition, a deal of well-preserved rather than dissolved ooids and skeletal debris were found out in thin sections (Figure 3(h)), which indicates that the patent water for calcite is rich in Ca2+ and CO32- ions and thereby ensures the integrity of these ooids and skeletal debris. So, there exist material sources for early calcite precipitation [50, 53].As the burial depth increases, the Es3 sandstones entered in the late eogenetic field characterized by acidic environment [6]. In this stage, mudstone beds adjacent to the Es3 sandstones began to generate and release organic acids by decarboxylation of organic matters due to a geotemperature close to 70°C [6, 25]. These processes not only led to secondary dissolution of feldspar but also resulted in early quartz cements [23]. Under microscope, there are abundant intragranular pores and/or even moldic pores evidencing the secondary dissolution of feldspar (Figure 3(f)). Unlike those early leaching-caused pores, these pores come with kaolinite aggregates close to dissolved feldspars (Figure 7(c)). From the perspective of porosity distribution, the ratio of secondary pores to the total pores is negatively correlated to the distance from the sand-body margin to center in individual sandstone near source rocks (Figure 11). This phenomenon indicates that the dissolving ability of organic acids gradually decreases with the increase in the distance between margin and center in individual sandstones [23, 50]. Dutton [53] documented feldspars had buffered acidic fluids and thus reduced solubility of Ca2+ irons and Mg2+ irons coming from adjacent source rocks, which resulted in nonferroan dolomite concentrated in sand-body margins.Figure 11
Distribution for the ratio of dissolved pores to total pores in individual sand-body deposited in brained channel with a thickness of 30.6 m versus the distance from test point to the contact interface between the sandstone and adjacent mudstone.According to Worden and Burley [6], twin characteristics of weak acidic environment and saturated SiO2 produced by feldspar dissolution are conducive to the precipitation of quartz cements. As the Es3 sandstones in the late eogenesis precisely met the above diagenetic environment conditions [25], the first generation of quartz cements (QogI) developed around protogenetic quartz grains as a response to the conditions and tended to take the forms of syntaxial euhedral overgrowths (Figure 4(g)) [6, 49]. With previous chlorite coatings having blocked, retarded, and even prevented nucleation for quartz growth, discrete overgrowths prevailed in the early stage and then interlocked with each other to form large overgrowths [52, 54].


#### 5.1.2. Mesogenetic Processes

Mesogenetic events occur at a temperature higher than 70°C in Es3 sandstones. These reactions include dissolution of feldspar, chemical compaction, formation of kaolinite aggregates, precipitation of the second generation of quartz overgrowth (QogII), and ankerite development.With the increase in burial and temperature, more and more organic acid and organic CO2 from Es3 source rocks by thermal decarboxylation of kerogen were released and injected into Es3 sandstones. So, the dissolution of feldspar in the late stage of eogenesis continued to mesogenetic period. On the other hand, a series of long and concave-convex contacts between detrital quartz grains developed widely, representing the typical chemical compaction with progressive burial (Figure 3(b)) [7, 55]. In the meantime, mechanical compaction of the Es3 sandstones turned gradually into weakened so that it had been subordinate to chemical compaction, which limited the liquidity of formation water and resulted in porosity reduction. And thus, a large amount of kaolinite aggregates coming from the locally supersaturated solution can only precipitate in the pore spaces near the dissolved feldspars (Figure 7(c)). Shelton [56] documented that kaolinite cements derived from crystallization of solution materials in pore water often precipitate as pore aggregates of infilling [57]. In addition, petrological observations show QogII developed around QogI and near concave-convex contacts (Figure 4(g)). Dissolution of feldspar and pressure solution of detrital quartz possibly account for SiO2 sources to a large extent [57–60]. Texturally, these QogIIs also presented syntaxial texture in coincidence with the QogIs, but far less than QogIs in abundance (Table 1). In addition, the existence of CO2 in formation water during the precipitation of QogIIs is proved by the fact that CO2 was detected in fluid inclusions by laser Raman spectroscopy (Figure 12). This detection, therefore, suggests feldspar dissolution in the Es3 sandstones indeed occurred in formation water containing both organic CO2 and organic acids.Figure 12
Laser Raman spectroscopy of fluid inclusions in quartz cements for the Es3 member sandstones.
.XRD shows mix-layered illite/smectite (I/S) is the most widespread clay minerals without smectite at all in the Es3 sandstones (Table 2, Figure 6). According to previous studies, there are two mechanisms, transformation of kaolinite and replacement of smectite, for illite development [57, 60, 61]. However, kaolinite developed very well in the pore systems and no evidence indicates conversion of kaolinite to illite. On the contrary, smectite was not detected at all by XRD and SEM (Table 2, Figure 6), which probably imply that those smectites have transformed to illite and/or transitional product of I/S. Moreover, many literatures documented that transformation of smectite to illite can occur in the temperature environment of mesogenesis [60, 62]. In fact, smectite has not yet been fully converted into illite, but in the stage of I/S (Table 2). Morphologically, flaky occurrences of I/S (Figure 7(a)) and illite (Figure 7(f)) definitely support early smectite as precursor, which is coincident with mesogenetic condition during burial [60].Quantitatively, blocky and poikilotopic ankerite is volumetrically predominated in Es3 sandstones (Figure 4(d)), filling in remnant intergranular pores and intensely replacing original detrital quartz (Figure 4(f)), feldspar, and early calcite cement (Figure 4(e)) in situ. Texturally, these ankerites not only engulfed, and thus postdated the QogII (Figure 4(g)) [49, 63], but also replaced feldspar and quartz partly or completely, leading to oversized patches in some cases (Figure 4(f)). Fortunately, some original occurrences of those detrital grains were preserved to some extent. In addition, the Th’s of two-phase fluid inclusions hosted in these ankerites concentrate in the range of 115.2°C to 130.5°C with an average of 96.0°C (Figure 9), which indicate the chronology for the mesogenesis [52, 64]. According to the preserved mineral remnants and textures, those strong replacements resulted directly in the change of lithologies from arkosic arenites and lithic arenites to subarkosic arenites and sublithic arenites, respectively (Figure 5). In addition, concomitants with replacement and dissolution of K-feldspar providing sufficient K+ ions in pore water lead to smectite transformation during the process of illitization [6]. Theoretically, pyrite formation requires Fe2+ and S- ions in a reducing environment (Figures 7(g) and 7(h)). The condition for ankerite can also satisfy the requirements for pyrite during the evolution of organic matter in mesogenetic time [65–67]. According to the analysis of diagenetic events, the paragenetic sequences of those Es3 sandstones are reconstructed (Figure 13) as follows.Figure 13
General paragenetic sequences of the Es3 sandstones deeply buried sandstone in Raoyang Sag Bohai Bay Basin.


### 5.2. Origin of Carbonate Cements

There are many studies focusing on the originations of carbonate cements in the past decades [7, 30, 53, 68, 69]. In those studies, the internal and external were concluded on the sources of carbonate cements both in terrestrial and marine sandstones [53]. Internal sources include the initial carbonate rock fragments, ooids, and skeletal debris, dissolving and reprecipitating in the host sandstones [53, 67, 70]. External sources include interbedded mudstones, bioclast-rich beds, and adjacent source rocks, transporting into sandstones from outside [50, 53, 71–73].Petrographic observations indicate a few of skeletal debris and ooids can be found out in the Es3 sandstones (Figure 3(h)). However, the abundances of these components are too low in negligible quantity to supply such a large volume of carbonate cements (Table 1). There is rare petrographic evidence showing that dissolution occurred in these ooids and thus not ruling out their possibilities as internal sources of carbonate cements [53]. Moreover, the positive correlation between the content of ooids and the content of total carbonate cements in the Es3 sandstones (Figure 14) indeed indicates their importance for carbonate cements. Even if the total volume of secondary pores resulted from the dissolution of these internal carbonate constituents, it would not account for such a significant volume of carbonate cement. As a result, external source inputs are considered the principle origin of carbonate cements.Figure 14
Relationship between content of carbonate cements and content of ooids in the Eocene Es3 sandstones.According to the existence of undissolved ooids and skeletal debris in samples (Figure3(h)), we infer that the primary sedimentary water had a high-level concentration of Ca2+ and CO32- (CO2) ions. On the other hand, with the increase in temperature during burial, the solubility of CaCO3 decreased as a response, which caused a constant imbalance in chemical equilibrium and thus resulted in a direct precipitation for early calcite cements from the pore water as an external source (Figures 4(a) and 4(b)). Regarding isotopic compositions, carbon isotopic data imply calcite cements derived from biogenic carbonate (Figure 10). The δ13CPDB value of calcites ranging from -0.7 to 1.0‰ in conjunction with the ooids and skeletal debris values of -1.2 and -1.1‰ (Table 3) indicates the main source of ooids and skeletal debris was modified by meteoric water for calcite cements [53, 74]. However, the skeletal debris and ooids that sourced the cement mainly come outside from the upper Es3 member developing lacustrine carbonate strata rich in skeletal debris and ooids due to the abundance constraint in Es3 sandstones [75, 76]. In addition, δ18OSMOW value of these calcites varies between 12.3‰ and 19.0‰—far less than the values of 23.0‰ and 23.2‰ for the skeletal debris (Table 3). But an average δ18OSMOW of -11.91‰ for the meteoric water has been estimated in previous study [77]. Thus, the skeletal debris, with a contribution of δ18O-depleted meteoric water, provide material sources for those early calcite cements which is consistent with the result by δ13C. Based on the empirical formula for determining marine limestone and freshwater limestone to Jurassic and younger strata proposed by Keith and Weber [78], the calculated Z value ranges from 114.69 to 122.18 with an average of 118.98 (Table 3). There are five Z values being more than 120 which indicate seawater has involved in the formation of calcite to a certain extent [79]. Therefore, the probable four sources including skeletal debris, ooids, meteoric water, and seawater jointly served as the originations for early calcite cements.Owing to the low volume of nonferroan dolomite in the Es3 sandstones (Table 1), it is hard to acquire adequate information for its origin. However, the δ13CPDB of -4.1‰ and δ18OSMOW of 14.3‰ (Table 3) likely suggest that the nonferroan dolomite cement precipitated from the liquids similar in oxygen isotopic composition to that of the calcite formation water but modified by the external acidic δ13C-depleted water during the late stage of eogenetic time [53]. When it comes to the extensively developed ankerites, distribution pattern of ankerite-cemented zones can reflect the source of ankerite from a macroscopic view to some extent [29]. Figure 15 shows that ankerite mainly concentrates in the margins of sand-bodies and gradually cuts down in the direction pointing to sand-body center. This distribution of ankerite suggests its origin from outside the Es3 sandstones, with preferential development and cementation in the margins of sand-bodies.Figure 15
Distribution for the content of carbonate cements in individual sand-body deposited in brained channel with a thickness of 30.6 m versus the distance from test point to the contact interface between the sandstone and adjacent mudstone.From the perspective of stable isotope, the carbon and oxygen isotopic data obtained for ankerite cements are much lower than those for early calcite cements (Table3). Experimentally, the δ13CPDB and δ18OSMOW of these δ13C-depleted ankerites in the Es3 sandstones, respectively, range from -10.0‰ to -1.2‰ and 10.1‰ to 19.4‰ (Table 3). Liu et al. [68] claimed carbon isotope for carbonate cements in sandstone is more positive than those for their origin by 9.0‰ to 10.0‰ because of the carbon isotope fractionation in diagenetic processes. The relatively δ13C-depleted carbon for ankerites indicates an organic source from the decarboxylation of organic matter with a negative δ13C down to -33.0‰ or -18.0‰ [68, 80]. In addition, the low δ18O value for ankerite is still coincident with calcite precipitation from meteoric fluids, but formed at a much higher temperature in keeping with the microthermometric results upon gradually progressive burial. The Th’s of the fluid inclusions in those authigenic ankerites concentrate in the range between 115.2°C and 135.5°C with an average of 96.0°C (Figure 9).In terms of geochemical elements, such more ankerite cements certainly require an abundant supply for Fe2+ ions. However, dissolution of ferromagnesian grains and breakdown of volcanic rock fragments are insufficient to offer the large amount of Fe2+ ions needed for ankerites [81, 82]. Berner [83] documented that the concentration on iron and organic matter varied synchronously in fine deposits. The existence of largely organic OC-Fe (organic carbon associated with reactive iron phases) macromolecular structures tends to dissolve, and thus, those Fe2+ ions succeeded the parent body of source rocks during iron reduction process in reducing condition. Upon continual burial of the Es3 source rocks containing a huge amount of organic matter, temperature increased gradually. So, adequate Fe2+ ion reserves were released into the formation water with the oxygen level in formation water becoming depleted [84]. In the meanwhile, with the alteration of clay minerals in source rocks as a response to the temperature increasing plus dissolution of ferromagnesian grains and volcanic rock fragments, Ca2+ and Mg2+ ions were offered for ankerite precipitation [48, 53, 57].


## 5.1. Diagenetic Events and Paragenetic Sequences

Diagenetic processes of the Es3 sandstones have undergone two diagenetic stages: eogenesis (with maximum burial depth of 1.0-2.0 km and maximum temperature of 30-70°C, approximately) and mesogenesis (with burial depth deeper than 1.0-2.0 km and temperature higher than 30-70°C) [6, 13]. Actually, it is impossible to precisely measure absolute time and duration of each diagenetic event in detail. However, paragenetic sequences during burial can be reconstructed approximately by considering the diagenetic environments and mutual textural relations between authigenic components and/or initial constituents [23, 48].


### 5.1.1. Eogenetic Processes

Prior to becoming sedimentary rocks, all sediments had suffered diagenetic alterations at or near the surface of sediment pile, which is mainly influenced by the intergranular fluids deriving from depositional environment in an open system [6, 49]. First of all, mechanical compaction, which is more effective at packing loose sediments and driving intergranular water expulsion in initial burial stage, took place gradually in response to the increasing vertical stress [5, 6, 50]. Then, these sediments have been subjected to mechanical and chemical weathering alterations soon after deposition in the arid to semiarid climate during Es3 period [26], which would inevitably lead to leaching of feldspar with respect to the flowing formation fluids by involving in infiltrated meteoric water [18, 51]. Petrographic observations show feldspars are often dissolved along cleavage significantly and thus create a mass of secondary pores (Figures 3(e) and 3(f)). At the same time, various authigenic clay minerals were produced, among which chlorite coatings formed firstly attaching to detrital grain surfaces, as there is not any other authigenic mineral existing in the space between the detrital grain and chlorite coating (Figure 7(d)), and mostly chlorite coatings contact directly with those detrital grains (Figure 7(e)). Additionally, these chlorite coatings not only protected original pores by enhancing the ability for resisting compaction but also served as barriers to retard the development of quartz overgrowths [49, 52]. Kaolinite is another important type of early clay mineral growing on the surfaces of detrital grains. Under SEM, these kaolinites had been modified with a low-level of euhedral texture (Figure 7(b)). Although these kaolinites were associated with feldspar leaching, yet they were removed timely and immediately in the flowing solution [30]. So, the random distribution of these kaolinites in samples was developed instead of concentrating in local position near secondary leaching pores [18, 30]. Except for early clay cements, calcite was a nonnegligible scenario in the eogenetic processes (Figure 4(b)). In some cases, those intergranular calcites characterized by fine microcrystal assemblage reach up to 29.2% in volume (Table 1 and Figure 4(a)). This is indicative of its early origin as only during the early stage of the eogenetic period can the sediments provide such spacious intergranular volumes for calcite development. On the other hand, these authigenic calcites directly cover the chlorite coatings or detrital grain surfaces in textural relations and thus postdate the authigenic chlorites (Figure 4(b)). In addition, a deal of well-preserved rather than dissolved ooids and skeletal debris were found out in thin sections (Figure 3(h)), which indicates that the patent water for calcite is rich in Ca2+ and CO32- ions and thereby ensures the integrity of these ooids and skeletal debris. So, there exist material sources for early calcite precipitation [50, 53].As the burial depth increases, the Es3 sandstones entered in the late eogenetic field characterized by acidic environment [6]. In this stage, mudstone beds adjacent to the Es3 sandstones began to generate and release organic acids by decarboxylation of organic matters due to a geotemperature close to 70°C [6, 25]. These processes not only led to secondary dissolution of feldspar but also resulted in early quartz cements [23]. Under microscope, there are abundant intragranular pores and/or even moldic pores evidencing the secondary dissolution of feldspar (Figure 3(f)). Unlike those early leaching-caused pores, these pores come with kaolinite aggregates close to dissolved feldspars (Figure 7(c)). From the perspective of porosity distribution, the ratio of secondary pores to the total pores is negatively correlated to the distance from the sand-body margin to center in individual sandstone near source rocks (Figure 11). This phenomenon indicates that the dissolving ability of organic acids gradually decreases with the increase in the distance between margin and center in individual sandstones [23, 50]. Dutton [53] documented feldspars had buffered acidic fluids and thus reduced solubility of Ca2+ irons and Mg2+ irons coming from adjacent source rocks, which resulted in nonferroan dolomite concentrated in sand-body margins.Figure 11
Distribution for the ratio of dissolved pores to total pores in individual sand-body deposited in brained channel with a thickness of 30.6 m versus the distance from test point to the contact interface between the sandstone and adjacent mudstone.According to Worden and Burley [6], twin characteristics of weak acidic environment and saturated SiO2 produced by feldspar dissolution are conducive to the precipitation of quartz cements. As the Es3 sandstones in the late eogenesis precisely met the above diagenetic environment conditions [25], the first generation of quartz cements (QogI) developed around protogenetic quartz grains as a response to the conditions and tended to take the forms of syntaxial euhedral overgrowths (Figure 4(g)) [6, 49]. With previous chlorite coatings having blocked, retarded, and even prevented nucleation for quartz growth, discrete overgrowths prevailed in the early stage and then interlocked with each other to form large overgrowths [52, 54].


### 5.1.2. Mesogenetic Processes

Mesogenetic events occur at a temperature higher than 70°C in Es3 sandstones. These reactions include dissolution of feldspar, chemical compaction, formation of kaolinite aggregates, precipitation of the second generation of quartz overgrowth (QogII), and ankerite development.With the increase in burial and temperature, more and more organic acid and organic CO2 from Es3 source rocks by thermal decarboxylation of kerogen were released and injected into Es3 sandstones. So, the dissolution of feldspar in the late stage of eogenesis continued to mesogenetic period. On the other hand, a series of long and concave-convex contacts between detrital quartz grains developed widely, representing the typical chemical compaction with progressive burial (Figure 3(b)) [7, 55]. In the meantime, mechanical compaction of the Es3 sandstones turned gradually into weakened so that it had been subordinate to chemical compaction, which limited the liquidity of formation water and resulted in porosity reduction. And thus, a large amount of kaolinite aggregates coming from the locally supersaturated solution can only precipitate in the pore spaces near the dissolved feldspars (Figure 7(c)). Shelton [56] documented that kaolinite cements derived from crystallization of solution materials in pore water often precipitate as pore aggregates of infilling [57]. In addition, petrological observations show QogII developed around QogI and near concave-convex contacts (Figure 4(g)). Dissolution of feldspar and pressure solution of detrital quartz possibly account for SiO2 sources to a large extent [57–60]. Texturally, these QogIIs also presented syntaxial texture in coincidence with the QogIs, but far less than QogIs in abundance (Table 1). In addition, the existence of CO2 in formation water during the precipitation of QogIIs is proved by the fact that CO2 was detected in fluid inclusions by laser Raman spectroscopy (Figure 12). This detection, therefore, suggests feldspar dissolution in the Es3 sandstones indeed occurred in formation water containing both organic CO2 and organic acids.Figure 12
Laser Raman spectroscopy of fluid inclusions in quartz cements for the Es3 member sandstones.
.XRD shows mix-layered illite/smectite (I/S) is the most widespread clay minerals without smectite at all in the Es3 sandstones (Table 2, Figure 6). According to previous studies, there are two mechanisms, transformation of kaolinite and replacement of smectite, for illite development [57, 60, 61]. However, kaolinite developed very well in the pore systems and no evidence indicates conversion of kaolinite to illite. On the contrary, smectite was not detected at all by XRD and SEM (Table 2, Figure 6), which probably imply that those smectites have transformed to illite and/or transitional product of I/S. Moreover, many literatures documented that transformation of smectite to illite can occur in the temperature environment of mesogenesis [60, 62]. In fact, smectite has not yet been fully converted into illite, but in the stage of I/S (Table 2). Morphologically, flaky occurrences of I/S (Figure 7(a)) and illite (Figure 7(f)) definitely support early smectite as precursor, which is coincident with mesogenetic condition during burial [60].Quantitatively, blocky and poikilotopic ankerite is volumetrically predominated in Es3 sandstones (Figure 4(d)), filling in remnant intergranular pores and intensely replacing original detrital quartz (Figure 4(f)), feldspar, and early calcite cement (Figure 4(e)) in situ. Texturally, these ankerites not only engulfed, and thus postdated the QogII (Figure 4(g)) [49, 63], but also replaced feldspar and quartz partly or completely, leading to oversized patches in some cases (Figure 4(f)). Fortunately, some original occurrences of those detrital grains were preserved to some extent. In addition, the Th’s of two-phase fluid inclusions hosted in these ankerites concentrate in the range of 115.2°C to 130.5°C with an average of 96.0°C (Figure 9), which indicate the chronology for the mesogenesis [52, 64]. According to the preserved mineral remnants and textures, those strong replacements resulted directly in the change of lithologies from arkosic arenites and lithic arenites to subarkosic arenites and sublithic arenites, respectively (Figure 5). In addition, concomitants with replacement and dissolution of K-feldspar providing sufficient K+ ions in pore water lead to smectite transformation during the process of illitization [6]. Theoretically, pyrite formation requires Fe2+ and S- ions in a reducing environment (Figures 7(g) and 7(h)). The condition for ankerite can also satisfy the requirements for pyrite during the evolution of organic matter in mesogenetic time [65–67]. According to the analysis of diagenetic events, the paragenetic sequences of those Es3 sandstones are reconstructed (Figure 13) as follows.Figure 13
General paragenetic sequences of the Es3 sandstones deeply buried sandstone in Raoyang Sag Bohai Bay Basin.


## 5.1.1. Eogenetic Processes

Prior to becoming sedimentary rocks, all sediments had suffered diagenetic alterations at or near the surface of sediment pile, which is mainly influenced by the intergranular fluids deriving from depositional environment in an open system [6, 49]. First of all, mechanical compaction, which is more effective at packing loose sediments and driving intergranular water expulsion in initial burial stage, took place gradually in response to the increasing vertical stress [5, 6, 50]. Then, these sediments have been subjected to mechanical and chemical weathering alterations soon after deposition in the arid to semiarid climate during Es3 period [26], which would inevitably lead to leaching of feldspar with respect to the flowing formation fluids by involving in infiltrated meteoric water [18, 51]. Petrographic observations show feldspars are often dissolved along cleavage significantly and thus create a mass of secondary pores (Figures 3(e) and 3(f)). At the same time, various authigenic clay minerals were produced, among which chlorite coatings formed firstly attaching to detrital grain surfaces, as there is not any other authigenic mineral existing in the space between the detrital grain and chlorite coating (Figure 7(d)), and mostly chlorite coatings contact directly with those detrital grains (Figure 7(e)). Additionally, these chlorite coatings not only protected original pores by enhancing the ability for resisting compaction but also served as barriers to retard the development of quartz overgrowths [49, 52]. Kaolinite is another important type of early clay mineral growing on the surfaces of detrital grains. Under SEM, these kaolinites had been modified with a low-level of euhedral texture (Figure 7(b)). Although these kaolinites were associated with feldspar leaching, yet they were removed timely and immediately in the flowing solution [30]. So, the random distribution of these kaolinites in samples was developed instead of concentrating in local position near secondary leaching pores [18, 30]. Except for early clay cements, calcite was a nonnegligible scenario in the eogenetic processes (Figure 4(b)). In some cases, those intergranular calcites characterized by fine microcrystal assemblage reach up to 29.2% in volume (Table 1 and Figure 4(a)). This is indicative of its early origin as only during the early stage of the eogenetic period can the sediments provide such spacious intergranular volumes for calcite development. On the other hand, these authigenic calcites directly cover the chlorite coatings or detrital grain surfaces in textural relations and thus postdate the authigenic chlorites (Figure 4(b)). In addition, a deal of well-preserved rather than dissolved ooids and skeletal debris were found out in thin sections (Figure 3(h)), which indicates that the patent water for calcite is rich in Ca2+ and CO32- ions and thereby ensures the integrity of these ooids and skeletal debris. So, there exist material sources for early calcite precipitation [50, 53].As the burial depth increases, the Es3 sandstones entered in the late eogenetic field characterized by acidic environment [6]. In this stage, mudstone beds adjacent to the Es3 sandstones began to generate and release organic acids by decarboxylation of organic matters due to a geotemperature close to 70°C [6, 25]. These processes not only led to secondary dissolution of feldspar but also resulted in early quartz cements [23]. Under microscope, there are abundant intragranular pores and/or even moldic pores evidencing the secondary dissolution of feldspar (Figure 3(f)). Unlike those early leaching-caused pores, these pores come with kaolinite aggregates close to dissolved feldspars (Figure 7(c)). From the perspective of porosity distribution, the ratio of secondary pores to the total pores is negatively correlated to the distance from the sand-body margin to center in individual sandstone near source rocks (Figure 11). This phenomenon indicates that the dissolving ability of organic acids gradually decreases with the increase in the distance between margin and center in individual sandstones [23, 50]. Dutton [53] documented feldspars had buffered acidic fluids and thus reduced solubility of Ca2+ irons and Mg2+ irons coming from adjacent source rocks, which resulted in nonferroan dolomite concentrated in sand-body margins.Figure 11
Distribution for the ratio of dissolved pores to total pores in individual sand-body deposited in brained channel with a thickness of 30.6 m versus the distance from test point to the contact interface between the sandstone and adjacent mudstone.According to Worden and Burley [6], twin characteristics of weak acidic environment and saturated SiO2 produced by feldspar dissolution are conducive to the precipitation of quartz cements. As the Es3 sandstones in the late eogenesis precisely met the above diagenetic environment conditions [25], the first generation of quartz cements (QogI) developed around protogenetic quartz grains as a response to the conditions and tended to take the forms of syntaxial euhedral overgrowths (Figure 4(g)) [6, 49]. With previous chlorite coatings having blocked, retarded, and even prevented nucleation for quartz growth, discrete overgrowths prevailed in the early stage and then interlocked with each other to form large overgrowths [52, 54].


## 5.1.2. Mesogenetic Processes

Mesogenetic events occur at a temperature higher than 70°C in Es3 sandstones. These reactions include dissolution of feldspar, chemical compaction, formation of kaolinite aggregates, precipitation of the second generation of quartz overgrowth (QogII), and ankerite development.With the increase in burial and temperature, more and more organic acid and organic CO2 from Es3 source rocks by thermal decarboxylation of kerogen were released and injected into Es3 sandstones. So, the dissolution of feldspar in the late stage of eogenesis continued to mesogenetic period. On the other hand, a series of long and concave-convex contacts between detrital quartz grains developed widely, representing the typical chemical compaction with progressive burial (Figure 3(b)) [7, 55]. In the meantime, mechanical compaction of the Es3 sandstones turned gradually into weakened so that it had been subordinate to chemical compaction, which limited the liquidity of formation water and resulted in porosity reduction. And thus, a large amount of kaolinite aggregates coming from the locally supersaturated solution can only precipitate in the pore spaces near the dissolved feldspars (Figure 7(c)). Shelton [56] documented that kaolinite cements derived from crystallization of solution materials in pore water often precipitate as pore aggregates of infilling [57]. In addition, petrological observations show QogII developed around QogI and near concave-convex contacts (Figure 4(g)). Dissolution of feldspar and pressure solution of detrital quartz possibly account for SiO2 sources to a large extent [57–60]. Texturally, these QogIIs also presented syntaxial texture in coincidence with the QogIs, but far less than QogIs in abundance (Table 1). In addition, the existence of CO2 in formation water during the precipitation of QogIIs is proved by the fact that CO2 was detected in fluid inclusions by laser Raman spectroscopy (Figure 12). This detection, therefore, suggests feldspar dissolution in the Es3 sandstones indeed occurred in formation water containing both organic CO2 and organic acids.Figure 12
Laser Raman spectroscopy of fluid inclusions in quartz cements for the Es3 member sandstones.
.XRD shows mix-layered illite/smectite (I/S) is the most widespread clay minerals without smectite at all in the Es3 sandstones (Table 2, Figure 6). According to previous studies, there are two mechanisms, transformation of kaolinite and replacement of smectite, for illite development [57, 60, 61]. However, kaolinite developed very well in the pore systems and no evidence indicates conversion of kaolinite to illite. On the contrary, smectite was not detected at all by XRD and SEM (Table 2, Figure 6), which probably imply that those smectites have transformed to illite and/or transitional product of I/S. Moreover, many literatures documented that transformation of smectite to illite can occur in the temperature environment of mesogenesis [60, 62]. In fact, smectite has not yet been fully converted into illite, but in the stage of I/S (Table 2). Morphologically, flaky occurrences of I/S (Figure 7(a)) and illite (Figure 7(f)) definitely support early smectite as precursor, which is coincident with mesogenetic condition during burial [60].Quantitatively, blocky and poikilotopic ankerite is volumetrically predominated in Es3 sandstones (Figure 4(d)), filling in remnant intergranular pores and intensely replacing original detrital quartz (Figure 4(f)), feldspar, and early calcite cement (Figure 4(e)) in situ. Texturally, these ankerites not only engulfed, and thus postdated the QogII (Figure 4(g)) [49, 63], but also replaced feldspar and quartz partly or completely, leading to oversized patches in some cases (Figure 4(f)). Fortunately, some original occurrences of those detrital grains were preserved to some extent. In addition, the Th’s of two-phase fluid inclusions hosted in these ankerites concentrate in the range of 115.2°C to 130.5°C with an average of 96.0°C (Figure 9), which indicate the chronology for the mesogenesis [52, 64]. According to the preserved mineral remnants and textures, those strong replacements resulted directly in the change of lithologies from arkosic arenites and lithic arenites to subarkosic arenites and sublithic arenites, respectively (Figure 5). In addition, concomitants with replacement and dissolution of K-feldspar providing sufficient K+ ions in pore water lead to smectite transformation during the process of illitization [6]. Theoretically, pyrite formation requires Fe2+ and S- ions in a reducing environment (Figures 7(g) and 7(h)). The condition for ankerite can also satisfy the requirements for pyrite during the evolution of organic matter in mesogenetic time [65–67]. According to the analysis of diagenetic events, the paragenetic sequences of those Es3 sandstones are reconstructed (Figure 13) as follows.Figure 13
General paragenetic sequences of the Es3 sandstones deeply buried sandstone in Raoyang Sag Bohai Bay Basin.


## 5.2. Origin of Carbonate Cements

There are many studies focusing on the originations of carbonate cements in the past decades [7, 30, 53, 68, 69]. In those studies, the internal and external were concluded on the sources of carbonate cements both in terrestrial and marine sandstones [53]. Internal sources include the initial carbonate rock fragments, ooids, and skeletal debris, dissolving and reprecipitating in the host sandstones [53, 67, 70]. External sources include interbedded mudstones, bioclast-rich beds, and adjacent source rocks, transporting into sandstones from outside [50, 53, 71–73].Petrographic observations indicate a few of skeletal debris and ooids can be found out in the Es3 sandstones (Figure 3(h)). However, the abundances of these components are too low in negligible quantity to supply such a large volume of carbonate cements (Table 1). There is rare petrographic evidence showing that dissolution occurred in these ooids and thus not ruling out their possibilities as internal sources of carbonate cements [53]. Moreover, the positive correlation between the content of ooids and the content of total carbonate cements in the Es3 sandstones (Figure 14) indeed indicates their importance for carbonate cements. Even if the total volume of secondary pores resulted from the dissolution of these internal carbonate constituents, it would not account for such a significant volume of carbonate cement. As a result, external source inputs are considered the principle origin of carbonate cements.Figure 14
Relationship between content of carbonate cements and content of ooids in the Eocene Es3 sandstones.According to the existence of undissolved ooids and skeletal debris in samples (Figure3(h)), we infer that the primary sedimentary water had a high-level concentration of Ca2+ and CO32- (CO2) ions. On the other hand, with the increase in temperature during burial, the solubility of CaCO3 decreased as a response, which caused a constant imbalance in chemical equilibrium and thus resulted in a direct precipitation for early calcite cements from the pore water as an external source (Figures 4(a) and 4(b)). Regarding isotopic compositions, carbon isotopic data imply calcite cements derived from biogenic carbonate (Figure 10). The δ13CPDB value of calcites ranging from -0.7 to 1.0‰ in conjunction with the ooids and skeletal debris values of -1.2 and -1.1‰ (Table 3) indicates the main source of ooids and skeletal debris was modified by meteoric water for calcite cements [53, 74]. However, the skeletal debris and ooids that sourced the cement mainly come outside from the upper Es3 member developing lacustrine carbonate strata rich in skeletal debris and ooids due to the abundance constraint in Es3 sandstones [75, 76]. In addition, δ18OSMOW value of these calcites varies between 12.3‰ and 19.0‰—far less than the values of 23.0‰ and 23.2‰ for the skeletal debris (Table 3). But an average δ18OSMOW of -11.91‰ for the meteoric water has been estimated in previous study [77]. Thus, the skeletal debris, with a contribution of δ18O-depleted meteoric water, provide material sources for those early calcite cements which is consistent with the result by δ13C. Based on the empirical formula for determining marine limestone and freshwater limestone to Jurassic and younger strata proposed by Keith and Weber [78], the calculated Z value ranges from 114.69 to 122.18 with an average of 118.98 (Table 3). There are five Z values being more than 120 which indicate seawater has involved in the formation of calcite to a certain extent [79]. Therefore, the probable four sources including skeletal debris, ooids, meteoric water, and seawater jointly served as the originations for early calcite cements.Owing to the low volume of nonferroan dolomite in the Es3 sandstones (Table 1), it is hard to acquire adequate information for its origin. However, the δ13CPDB of -4.1‰ and δ18OSMOW of 14.3‰ (Table 3) likely suggest that the nonferroan dolomite cement precipitated from the liquids similar in oxygen isotopic composition to that of the calcite formation water but modified by the external acidic δ13C-depleted water during the late stage of eogenetic time [53]. When it comes to the extensively developed ankerites, distribution pattern of ankerite-cemented zones can reflect the source of ankerite from a macroscopic view to some extent [29]. Figure 15 shows that ankerite mainly concentrates in the margins of sand-bodies and gradually cuts down in the direction pointing to sand-body center. This distribution of ankerite suggests its origin from outside the Es3 sandstones, with preferential development and cementation in the margins of sand-bodies.Figure 15
Distribution for the content of carbonate cements in individual sand-body deposited in brained channel with a thickness of 30.6 m versus the distance from test point to the contact interface between the sandstone and adjacent mudstone.From the perspective of stable isotope, the carbon and oxygen isotopic data obtained for ankerite cements are much lower than those for early calcite cements (Table3). Experimentally, the δ13CPDB and δ18OSMOW of these δ13C-depleted ankerites in the Es3 sandstones, respectively, range from -10.0‰ to -1.2‰ and 10.1‰ to 19.4‰ (Table 3). Liu et al. [68] claimed carbon isotope for carbonate cements in sandstone is more positive than those for their origin by 9.0‰ to 10.0‰ because of the carbon isotope fractionation in diagenetic processes. The relatively δ13C-depleted carbon for ankerites indicates an organic source from the decarboxylation of organic matter with a negative δ13C down to -33.0‰ or -18.0‰ [68, 80]. In addition, the low δ18O value for ankerite is still coincident with calcite precipitation from meteoric fluids, but formed at a much higher temperature in keeping with the microthermometric results upon gradually progressive burial. The Th’s of the fluid inclusions in those authigenic ankerites concentrate in the range between 115.2°C and 135.5°C with an average of 96.0°C (Figure 9).In terms of geochemical elements, such more ankerite cements certainly require an abundant supply for Fe2+ ions. However, dissolution of ferromagnesian grains and breakdown of volcanic rock fragments are insufficient to offer the large amount of Fe2+ ions needed for ankerites [81, 82]. Berner [83] documented that the concentration on iron and organic matter varied synchronously in fine deposits. The existence of largely organic OC-Fe (organic carbon associated with reactive iron phases) macromolecular structures tends to dissolve, and thus, those Fe2+ ions succeeded the parent body of source rocks during iron reduction process in reducing condition. Upon continual burial of the Es3 source rocks containing a huge amount of organic matter, temperature increased gradually. So, adequate Fe2+ ion reserves were released into the formation water with the oxygen level in formation water becoming depleted [84]. In the meanwhile, with the alteration of clay minerals in source rocks as a response to the temperature increasing plus dissolution of ferromagnesian grains and volcanic rock fragments, Ca2+ and Mg2+ ions were offered for ankerite precipitation [48, 53, 57].


## 6. Conclusions

(1)
The deeply burial Es3 sandstones are mostly subangular-to-subrounded lithic arkoses and feldspathic litharenites with a fine to medium grain size and poor to moderate sorting, which were actually derived from arkoses and lithic arkoses, respectively(2)
The Es3 sandstones have undergone two diagenetic episodes of eogenesis and mesogenesis. Eogenetic events that were identified include mechanical compaction, leaching of feldspar, development of chlorite coating and kaolinite, precipitation of the first generation of quartz overgrowth, dissolution of feldspar, and precipitation of calcite and nonferroan dolomite cement. Mesogenetic alterations include chemical compaction, precipitation of kaolinite aggregate and the second generation of quartz overgrowth, precipitation of ankerite, transformation of I/S and illite, and formation of pyrite(3)
Carbonate cements are the most major pore filling components. For calcite, skeletal debris and ooids in adjacent carbonate beds combined with meteoric water and seawater from outside jointly served as the carbon sources; for nonferroan dolomite, it directly precipitated in the diagenetic environment with oxygen isotopic composition similar to composition to that of the calcite but modified by the external acidicδ13C-depleted water; for the most widespread ankerite, it mainly originated from the Es3 source rocks with effective feldspar buffer action for the acidic fluids along the margins of the Es3 sandstones. In addition, the other necessary elements such as Fe2+, Ca2+, and Mg2+ ions also come from organic matter and clay minerals during thermal maturation of source rocks



---

*Source: 8728432-2020-11-20.xml*