Next Article in Journal
A Case Study of the Radon Hazard at the Boundary of a Coal Minefield
Next Article in Special Issue
An Analysis of Silurian Paleo–Tethys Hydrocarbon Source Rock Characteristics in North Africa, the Middle East, and South China
Previous Article in Journal
Application-Oriented Data Analytics in Large-Scale Metal Sheet Bending
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Applied Sciences
Volume 13
Issue 24
10.3390/app132413186
applsci-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles thumb_up
...
Endorse textsms
...
Comment
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

Diagenesis of the Permian Fengcheng Formation in the Mahu Sag, Junggar Basin, China

by
Bin Bai
1,*,
Jiwei Liang
2,
Chaocheng Dai
3,
Wenjun He
4,
Ying Bai
1,
Xiaobin Chang
2,
Meng Zheng
2,
Hanlin Li
2 and
Hao Zong
2
1
Research Institute of Petroleum Exploration & Development, Beijing 100083, China
2
School of Earth Sciences and Resources, Chang’an University, Xi’an 710054, China
3
School of Earth Sciences, East China University of Technology, Nanchang 330013, China
4
Research Institute of Exploration and Development, Xinjiang Oilfield Company, PetroChina, Karamay 834000, China
*
Author to whom correspondence should be addressed.
Appl. Sci. 2023, 13(24), 13186; https://doi.org/10.3390/app132413186
Submission received: 19 October 2023 / Revised: 15 November 2023 / Accepted: 29 November 2023 / Published: 12 December 2023
(This article belongs to the Special Issue The Exploration and Development of Unconventional Hydrocarbon Resources, 2nd Volume)
Browse Figures
Versions Notes

Abstract

:
The Fengcheng Formation in the Mahu sag of the Junggar Basin was primarily composed of detritus, pyroclastic material, carbonates, and evaporites. In order to establish the diagenesis pathways of the Fengcheng Formation, some methods of polarized light microscope, SEM, CL, EPMA, LR, and fluid inclusion analysis were applied to discuss the diagenesis process. The results showed the following: (a) The formation of an alkaline lake was the result of the influence of a high concentration of sodium-rich sources, and it led to the preservation of alkaline minerals in the stratum. (b) After the sediments were buried, three mineral assemblages were formed in the Fengcheng Formation, which are carbonate mineral assemblages (i.e., calcite + ferreous dolomite), reedmergnerite and carbonate mineral assemblages (i.e., reedmergnerite + calcite + ferreous dolomite), and reedmergnerite and alkaline mineral assemblages (i.e., reedmergnerite + shortite + trona), respectively. (c) According to the homogenization temperature of reedmergnerite primary fluid inclusions, the alkaline diagenesis of Fengcheng Formation was divided into an early stage (≤100 °C) and a middle stage (>100 °C), respectively. The earlier stage is marked by the formation of ferrous saddle dolomite, quartz dissolution, and the agglutination of laumontite. These processes occurred under normal burial conditions. The latter is marked by the reedmergnerite’s appearance, which is correlated with the deep hydrothermal activity controlled by faults. (d) Based on sedimentary and diagenetic factors, including climate, provenance, diagenetic surroundings, and the action of subsurface fluid, the alkaline deposition-diagenesis model for shale series in four stages of the Fengcheng Formation was established.

1. Introduction

Traditional early and middle diagenesis is mainly conducted in acidic diagenetic environments, which are characterized by carbonate mineral, feldspar, and clay minerals being in an unstable state and easy to be dissolved [1,2,3,4,5]. When the reservoir experiences an alkaline diagenetic environment, reservoir property is often changed due to the role of alkaline formation water, quartz dissolution, feldspar enlargement, and carbonate mineral replacement becoming the most distinctive diagenetic phenomena [6,7,8,9,10,11]. The theory of alkaline diagenesis has enriched, improved, and deepened the traditional theory of diagenesis. At present, the understanding of alkaline diagenesis is relatively insufficient compared to traditional diagenesis. The conditions of alkaline diagenesis generally include a sedimentary environment, climate, organic acids, and thermal fluid evolution [12,13]. Alkaline diagenesis can have constructive effects on reservoirs [14,15]. For example, mica interlaminar pores and albite pores formed under the action of alkaline fluids are good oil storage spaces. The diagenetic phenomena of alkaline diagenesis are diverse, including alkali lacustrine salt rocks [16], alkaline evaporative salt minerals [17], and quartz dissolution under the action of alkaline groundwater [18]. In addition, alkaline diagenesis may also provide a new explanation for the silicification of metal deposits, the origin of siliceous cementation, and the reddening and fragmentation of rocks [11,12,13,14,15,16,17,18,19].
The Junggar Basin is located in northwestern China (Figure 1a), with an area of about 1393 square kilometers [20]. The basin is divided into six first-level structural units: Ulungu sag, Luliang uplift, Western uplift, Central sag, Eastern uplift, and North Tianshan thrust band [21] (Figure 1a). The Mahu sag, located northwest of the Central sag of the Junggar Basin in an NE trend, is the most petroliferous sag (Figure 1). The most important source rock in the northwestern part of the Mahu sag is the lower Permian Fengcheng Formation [3,21,22]. The Fengcheng Formation consists of a mixed shale series comprising carbonate rocks, alkaline intermediate to basic volcanic rocks, and terrigenous detrital rocks. It contains alkaline minerals such as kanemite, bradleyite, and eitelite, suggesting formation in an alkaline lake environment [23]. The rocks of the Fengcheng Formation also contain bands and clumps of the uncommon mineral reedmergnerite [Na(BSi3O8)], indicating that it has undergone complex diagenetic processes [4,5,6]. The Fengcheng Formation is a fair-to-good source rock development horizon with high organic matter content, which has the characteristics of multi-phase hydrocarbon generation peak and large-area hydrocarbon generation [23,24]. Meanwhile, the Fengcheng Formation has good exploration prospects and development value for oil and gas exploration, which has been widely concerned in the oil field recently. Studies show that the alkali lake of the Fengcheng Formation has experienced five stages of drought-wet-dry-heat-continuous dry-heat-humid [25], forming major reservoir types, including dolomite, clastic rock, and volcanic rock, and the formation of alkaline minerals is closely related to the evaporative salinization of lake brine [26]. The study of the alkaline lake environment and its diagenesis is still in the initial stage and needs to be further studied. Focused on the Fengcheng Formation, this study tried to obtain (1) the petrological and mineralogical characteristics, (2) diagenetic types, (3) and sedimentary diagenetic models, and this study is helpful for promoting the theoretical innovation of the Fengcheng Formation for further oil and gas exploration purposes.

2. Geological Setting and Samples

The northeastern part of the Junggar Basin is close to the Qingridi Mountains and Kelamei Mountains, the southern part is adjacent to the Tianshan Mountains, and the northwest/western parts are the Delun Mountains, Halaalate Mountains, and Zaire Mountains, which are nearly triangular, with a sharp southeast and a wide northwest (Figure 1a). The Junggar Basin, an important part of the Central Asian Orogenic Belt [21], belongs to the superimposed basin [28,29], whose Late Devonian/Early Carboniferous contribution was rift basins, while the Late Carboniferous/Permian period formed foreland basins, and the Triassic/Paleogene periods formed intracontinental depression basins [27]. From the Early Paleozoic to the end of the Late Paleozoic Carboniferous period, the Junggar Basin had a long-term multi-island oceanic paleogeographic pattern with discrete island arcs and ocean basins arranged alternately [28], and with the evolution of the Paleo-Asian Ocean Basin, the marine area gradually diminished [28]. When the Jiamuhe Formation was deposited in the Early Permian period, some areas in the basin evolved into residual marine facies [30], until the Early Permian Fengcheng Formation. During this period, the Fengcheng, Wuerhe, and Xiazijie areas in the Mahu sag evolved into salinized lake basin facies after the closure of the residual sea [25].
The Mahu sag is located in the northwest part of the Central sag of the Junggar Basin in an NE trend. It is a secondary structural unit in the basin [28], with a length of about 100 km, a width of about 50 km, and an area of about 5000 square kilometers [30]. The tectonic unit dips gently to the southeast as a whole [31] and is one of the sags with the richest oil and gas content in the basin [32,33]. The Mahu sag is adjacent to the Kebai and Wuxia large fault zones in the northwest [34], the Yingxi sag in the east, the Dabasong-Xiayan uplift in the southeast, and the Zhongguai uplift in the southwest [25,35] (Figure 1a), and it was developed on the pre-Carboniferous folded basement [27]. The Lower Permian Fengcheng Formation is the main source of rock formation in the Mahu sag [36], with a maximum formation thickness of 1500 m [26]. It is the oldest alkali lacustrine source rock discovered in the world so far [37]. It experienced three periods of hydrocarbon generation peaks: Late Permian, Late Triassic, and Late Cretaceous [29], and the generated oil and gas were accumulated in the Fengcheng Formation and its overlying Wuerhe Formation and Baikouquan Formation [38]. According to the rock combination, from bottom to top, the Fengcheng Formation can be divided into three sections, including Feng 1, Feng 2, and Feng 3. The Feng 1 Member mainly develops volcanic rocks, the Feng 2 Member develops mudstone and carbonate rocks, which are rich in reedmergnerite, and the Feng 3 Member mainly develops terrigenous detrital rocks (Figure 1b,c).

3. Analytical Methods

Castings and multi-purpose slices of exploratory well cores such as FN1, FN14, AK-1, and MH7 are used as the main experimental objects.

3.1. Morphology and Microscopic Features Analyses

The multi-purpose and cast thin sections were analyzed by a polarized light microscope to obtain key information such as the type, morphology, and mutual relationship between minerals in thin sections, and the pores were observed. At the same time, the microscopic features of minerals such as quartz, zeolite, and clay were recorded under the scanning electron microscope (SEM), and the ring-band structure of carbonate minerals was observed in the cathode luminescence (CL) test. The scanning electron microscope (SEM-QUANTA650, FEI Co., USA) experiment was completed in the Mineralization and Dynamics Laboratory of Chang’an University, and the cathode luminescence (CL 8200mk5-2, Germany) test was carried out in the Xi’an National Engineering Laboratory for Low Permeability Oil and Gas Field Exploration and Development.

3.2. Compositions of Minerals Analyses

For Mg-Ca carbonate minerals and special alkaline minerals widely distributed in thin slices, electron probe microanalysis (EPMA) was used to determine the composition of carbonate minerals, to determine the specific content of each component, and to assist in determining the type of alkaline minerals. Because the reedmergnerite in alkaline minerals is special, the laser Raman method (LR) was used to analyze it. The LinkamTHMS600 (Britain) geological cold and hot platform was used for testing the homogenization temperature of reedmergnerite primary fluid inclusions. The electron probe (EPMA-JXA8100, Jeol, Japan) experiment was completed in the Mineralization and Dynamics Laboratory of Chang’an University, and the laser Raman (Renishaw inVia type confocal laser Raman spectrometer, Britain) test experiment was completed in the Xi’an Institute of Geology and Mineral Resources.
In order to avoid the interference of external substances and assure the accuracy of the experimental results, all core slices were stored in slice boxes before the experiment, and the experimental process was strictly operated according to the standard [4,5,6,7,8].

4. Results

4.1. Petrological Characteristics

The Fengcheng Formation is a set of mixed shale series composed of alkaline intermediate-basic volcanic rocks, carbonate rocks, and terrigenous clastic rocks.

4.1.1. Volcanic Rock

Volcanic rocks are one of the rock types in the study area, which were mainly developed in the Fengcheng 1 Member, and they can be divided into three categories: subvolcanics, volcanic lava, and volcanic clastic rocks (Figure 2). Subvolcanics are also divided into basaltic porphyrite and esitic porphyrite. Basalt, andesitic rock, and trachyte could be determined from volcanic lava. Volcanic clastic rocks mainly consist of tuff and breccia. Rock and mineral identification and previous studies showed that the volcanic rocks are mainly intermediate-basic. The discovery of the silica-alkali diagram and titan pyroxene (Table 1) of volcanic rocks showed that the volcanic rocks of the Fengcheng Formation are alkaline.

4.1.2. Carbonate Rocks

Carbonate rocks are mainly dolostone and argillaceous dolomite developed in the second member of the Fengcheng Formation, while only thin or small carbonate lenses are found in the Fengcheng 1 Member and the Fengcheng 3 Member (Figure 1b,c). The middle striation of dolomite is developed, and most is interbedded with argillaceous rocks. Dolomites are mostly fine-grained with microcrystalline clays, and the content of dolomite is 45–65 wt.% (atomic percent). A small amount of volcanic tuff, including volcanic eruptions and terrigenous, fine-grained tuff debris, is visible in some dolomites [39].

4.1.3. Terrigenous Clastic Rocks

The terrigenous clastic rocks are conglomerate, sandstone, and mudstone. Conglomerate and sandstone are developed in the Fengcheng 3 Member. Dolomite particles and volcanic tuff are common in the rocks. The closer the lake basin edge is, the larger the particle size is, and the debris may mainly come from the Zaire Mountain in the west of the Mahu sag [40,41]. Mudstone is very common in the Feng 1, Feng 2, and Feng 3 sections. The thickness of Feng 2 is large, and it is rich in bacteria and organic algae matter [26,28]. It is the main source rock position of the Fengcheng Formation. There are seasonal laminae [40,41,42]. Microcrystalline calcite, in some areas of mudstone, experienced dolomitization and transformed to dolomite, with lake water as the Mg source.

4.2. Mineralogical Characteristics

Fe-bearing dolomite, calcite, and other minerals are significant diagenetic components of the shale series in the Fengcheng Formation within the Mahu sag. Studying the relationship between them is of great significance for the classification of alkaline diagenesis. The Fengcheng Formation in this area is preliminarily divided into three mineral assemblages: carbonate mineral assemblage, borosilicate-carbonate mineral assemblage, and borosilicate-alkaline mineral assemblage.
The dolomite of the Fengcheng Formation generally contains iron (Table 1), with the highest iron content of 13% and an average of 8.5% [43]. Fe2+ does not replace half of Mg2+; thus, it is iron dolomite. There are three forms of iron dolomite: mud microcrystal layered (Figure 3a), powder crystal block (Figure 3b,c), and snowflake (Figure 3d,e). Under cathode luminescence, the band structure of mud-microcrystalline layered iron dolomite is only occasionally seen. The fine-grained block and snowflake-like iron dolomites have a clear ring structure, which can be divided into irregular undulate type I ring combination (Figure 3e) and rhombic type II ring combination (Figure 3f). The edge morphology of the outermost ring of the type II ring combination is different, mostly in a straight shape (Figure 3f), and occasionally in a serrated or clamshell shape, which may be caused by late corrosion events [35,36]. It is difficult to see pure calcite in the Fengcheng Formation. Calcite has been replaced by dolomite or iron dolomite, and a small part has been replaced by sodium borosilicate (Figure 3g). Reedmergnerite [Na(BSi3O8)] is a rare diagenetic mineral, mainly distributed in the Feng 1 and Feng 2 Members, and it often coexists with carbonate minerals. After calcite dolomitization, iron dolomite was replaced by borosilicate; some reedmergnerite developed metasomatic relict texture, and carbonate minerals remained in the minerals (Figure 3h). It is inferred that the formation age of borosilicate is later than that of carbonate minerals. The reedmergnerite can be divided into two types according to the degree of self-shape: wedge-shaped reedmergnerite with a high degree of self-shape and diamond-plate-shaped reedmergnerite with a low degree of self-shape (Figure 4b) and wreck-shaped reedmergnerite (Figure 3h). The former is mostly aggregated growth (Figure 4a), while the latter is mostly scattered in the matrix. The mineral is not pure inside, and the mineral edge is jagged or irregularly radial.
Under the microscope, the butterfly-shaped twinned crystals and a group of complete cleavages can be seen in the high degree of self-shaped reedmergnerite. Under the cathodoluminescence, reedmergnerite emits blue light with different intensities (Figure 3c). Since boron element is located at the lowest detection ability of electron probe microanalyzer (EPMA) [44], the total content of each component in reedmergnerite measured in this paper was about 79–85%, less than 100% (Table 2). The difference may be that the content of B2O5 and the content of B2O5 after treatment are close to the standard content of B2O5 in reedmergnerite [45]. In order to enhance credibility and accuracy, the laser Raman (LR) method was used to test the reedmergnerite. The test spectra showed that the transverse coordinates of the four characteristic peaks were 230 cm−1, 600 cm−1, 1000 cm−1, and 1600 cm−1, respectively. The transverse coordinate of the main peak was 600 cm−1, which was similar to the characteristics of the Reedmergnerite Raman spectra [46] (Figure 5).
Reedmergnerite often appears with alkaline minerals. Due to the limitation of the number of drilling wells, in the samples of the Fengcheng Formation, it was found that wollastonite was mainly symbiotic with trona and shortite (Figure 4d,e). From the metasomatism relationship between them, for example, reedmergnerite starts to replace the shortite from the edge (Figure 4d), and it can be seen that the formation of reedmergnerite was later than alkaline minerals.

4.3. Homogenization Temperature of Reedmergnerite Primary Fluid Inclusions

According to the phase combination and microscopic fluorescence characteristics of fluid inclusions at room temperature, the fluid inclusions of reedmergnerite can be divided into five categories: (1) liquid-only inclusions (L-O) in a single liquid phase without visible bubbles; (2) liquid-dominated two-phase inclusions (L-D) with a gas–liquid ratio less than 50%; (3) single-liquid phase oil inclusions emitting blue light under fluorescence; (4) gas–liquid two-phase oil inclusions with a gas–liquid ratio of less than 50% emitting blue light under fluorescence; (5) oil inclusions emitting yellow light under fluorescence. The occurrence of fluid inclusions mainly includes the following four types: (1) The inclusions in the growth zone (GZ) often exhibit mineral growth characteristics (Figure 6a,b), and these inclusions are considered reliable primary inclusions. Fluid inclusions within the same growth zone belong to the same associations of fluid inclusions (FIA). (2) Clustered inclusions (Figure 6c) are usually clustered in a relatively small area, and clustered inclusions may be primary or secondary. When they are primary inclusions, they belong to the same FIA. (3) Random population (RP) inclusions, which are randomly and directionally distributed in a relatively large area (Figure 6d), are of unknown origin and may be either primary or secondary. In any case, such inclusions do not belong to the same FIA. (4) The inclusion in Long Trail (LT) refers to a healing crack that cuts through the mineral boundary (Figure 6e,f), the inclusion produced as a healing crack is considered a typical secondary inclusion, and the inclusion produced in the same healing crack belongs to one FIA [47].
Through systematic analysis of fluid inclusion petrography, the inclusions in the study area mainly exhibit the following five types of associations: (1) Rich liquid two-phase saline inclusions with relatively consistent gas–liquid ratios were detected in the growth zone of reedmergnerite minerals (Figure 6b). (2) A rich liquid phase two-phase brine inclusion was detected in the long healing crack of cut borosilicate (Figure 6f). (3) The long healing crack of cut borosilicate was detected as a rich liquid-phase two-phase oil inclusion with green fluorescence (Figure 6g,h). (4) Rich liquid phase two-phase oil inclusions with yellow and blue fluorescence were detected in multiple long healing cracks of cut borosilicate (Figure 6i). (5) Long healing cracks in cut borosilicate were detected, with yellow fluorescent two-phase oil inclusions in the rich liquid phase and two-phase saline inclusions in the rich liquid phase.
A total of 15 L-D fluid inclusions with relatively consistent gas–liquid ratios were detected in the growth band, forming three FIAs. The three FIAs showed consistent temperature measurement data (Table 3), and the homogenization temperature (Th) range of 15 L-D fluid inclusions was 100–116 °C (Figure 7).

5. Discussion

5.1. Types of Alkaline Lake Diagenesis and Their Causes

Diagenetic minerals, such as iron dolomite and laumontite, can form under normal burial temperature conditions. However, the formation of reedmergnerite occurs at relatively high temperatures [42,43]. According to the homogenization temperature of reedmergnerite primary fluid inclusions, alkaline diagenesis of the Fengcheng Formation was divided into two stages, which are early stage (≤100 °C) and middle stage (>100), with the early stage corresponding to low-temperature alkaline diagenesis and middle stage corresponding to medium-high-temperature alkaline diagenesis. The manifestations of low-temperature alkaline diagenesis include the formation of iron dolomite rings, quartz dissolution, and cementation of laumontite, and the appearance of reedmergnerite marked the medium-high-temperature alkaline diagenesis.

5.1.1. Indicative Significance of Iron Dolomite Ring

Because the content of Fe2+ is closely related to the CL luminescence intensity of the band [30,43,44], it is important to analyze the source of Fe2+. There are two sources of Fe in Fengcheng Formation iron dolomite: (1) The upwelling of marine brine due to the action of capillary force brought a large amount of Fe. The residual marine brine of the Jiamuhe Formation under the Fengcheng Formation invaded [48], bringing abundant elements such as Fe, Mn, and Mg [49]. (2) Meanwhile, the various microorganisms in the Fengcheng Formation are beneficial for the enrichment of iron elements [17,24]. (3) Fe elements contributed with medium basic volcanic ash. Volcanic ashes are widely distributed in Fengcheng Formation [48], and medium basic volcanic ashes contain a large amount of Mg, Fe, and other elements [50], which release a large amount of Fe2+ in the process of the devitrification of volcanic glasses.

5.1.2. Quartz Dissolution

Quartz dissolution is a typical alkaline diagenetic phenomenon [51,52]. Three different quartz dissolution phenomena were found in the core thin sections of the Fengcheng Formation: (1) the edge of quartz particles is dissolved, and it becomes serrated or bay-shaped (Figure 4f); (2) the quartz particles are corroded inside, and microscopic dense “honeycomb” corrosion pits can be seen on the mineral surface in SEM tests (Figure 4g); (3) quartz grains develop an irregular linear distribution of fractures, and some of the fractures are locally widened by further corrosion.
The dissolution of quartz in the Fengcheng Formation was affected by Na+, temperature, and alkalinity, and it occurred during the burial diagenetic period. Quartz dissolution is closely related to the alkaline diagenetic environment [1,17,51,53], especially with the alkaline cation Na+, which can form sodium silicate on the surface of quartz particles through hydration reactions, and then, they crack to cause quartz erosion [54,55,56]. The Fengcheng Formation rocks were formed in an alkaline lake environment [39,40,41,42,43,44,56,57]. The Fengcheng Formation volcanic rocks are sodium-rich volcanic rocks, and the content of Na2O in the volcanic rocks is much higher than that of K2O [58]. The Na element mainly exists in albite. The albite content in the volcanic rocks of the Fengcheng Formation is high [33], and the hydrolysis of albite increases the content of Na+, which causes the cations in the alkaline lake water to be dominated by Na+ [40]. The alkaline diagenetic environment rich in Na+ is favorable for quartz dissolution because the high Na+ content increases the probability of Na+ forming complexes on the quartz surface.
Under the same conditions, the dissolution rate of quartz at a high temperature (430 °C) is 11 orders of magnitude faster than that at a relatively low temperature (25 °C) [59], that is. High temperature is beneficial for the dissolution of quartz. In addition, the pH value also affects the dissolution of quartz. When the predecessors conducted hydrothermal experiments on the dissolution of quartz in an alkaline environment at a temperature of 130 °C and a pH value of 9.5, the quartz was significantly dissolved [52]. Therefore, the ground temperature was calculated according to the burial depth of the Fengcheng Formation, and it was concluded that such temperature conditions can be satisfied [59,60]. The pH value of the alkaline lake during the deposition of the Fengcheng Formation was in the range of 9–11 [25]. During the diagenetic stage, the alkalinity decreased, but the temperature increased. The temperature change had a greater impact on the quartz dissolution than the pH change [52]. Therefore, the Fengcheng Formation has the condition of quartz dissolution in a burial alkaline environment. In addition, due to the fact that quartz dissolution is positively correlated with Na+, the catalytic activity of the alkaline cation Na+ increases with the increase of alkalinity [50,58], and the increase of alkalinity can promote the dissolution of quartz. Regarding temperature and alkalinity, the dissolution of quartz is intensified with the rise of temperature in the middle- and high-temperature alkaline diagenetic stage. For example, the serrate dissolution of quartz edge is intensified and then becomes harbored, and the local dissolution of internal cracks in quartz minerals is intensified and widened.

5.1.3. Cementation of Laumontite

The laumontite in the Fengcheng Formation rocks mostly exists in the state of sheet-like cement (Figure 3h), which is an authigenic aluminosilicate mineral with a high content of Ca2+ formed in a neutral-alkaline environment, and the corresponding pH value is mostly 7–10 [61]. This type of zeolite cementation is closely related to the properties of volcanic materials and their hydrolysis [62,63]. As the stratum was buried and the temperature of the stratum rose, a large number of low-temperature unstable minerals contained in the intermediate–basic volcanic rocks (substances) were hydrolyzed to form laumontite cement in an alkaline environment [64]. With the evolution of organic matter in the Fengcheng Formation, a large amount of CO2 and short-chain organic fatty acids were released [64]. The atmospheric water infiltrated along the Kebai-Wuxia fault belt, and pore water was formed by the dehydration of clay minerals [65]. Under the combined action, the early cemented laumontite was dissolutive.

5.1.4. Formation of Reedmergnerite

The appearance of reedmergnerite marks the middle-high temperature alkaline diagenesis of the Fengcheng Formation, and its formation is closely related to the hydrothermal fluid. The main evidence is as follows: (1) During the period of the Fengcheng Formation, different rare earth element distribution models showed that the fluids mainly came from endogenous fluids in different parts, including subduction zones, crustal, and mantle sources, and the boron required for reedmergnerite mainly came from deep alkaline hydrothermal fluids [56,66]. (2) The measurement of boron isotope δ11B showed that the fluids of different forms of reedmergnerite in the Fengcheng Formation were from the same source, and the fluid may come from deep hydrothermal sources [56]. (3) Reedmergnerite is widely developed near the fault, and during the Fengcheng Formation, regarding the volcanic activity [67], boron-rich hydrothermal fluids affected by volcanic activity could migrate along developed fault networks. (4) Reedmergnerite was formed in a closed alkaline lake environment [41], and it was not easy for enthetic materials to enter the lake basin through relatively normal and gentle migration. The hydrothermal fluid in the deep is more capable of entering this closed environment under the external force of the huge energy [56], bringing the required substances. (5) The hydrothermal fluid can provide a sufficient reaction temperature, which can reach the experimental temperature required for the synthesis of reedmergnerite [46,47], while the reedmergnerite in the Fengcheng Formation was developed in the Feng 2, with a burial depth greater than 3000 m [56], and in 2018, Rao Song studied the thermal history recovery characteristics of the Junggar Basin by using paleo-temperature scale methods, such as vitrinite reflectance and fission track [60], and found that the geothermal gradient of the Fengcheng Formation was 5–3 °C/100 m. The formation temperature of the reedmergnerite development layer was about 140 °C (the average geothermal gradient is 4 °C, and the annual average temperature is about 20 °C), which cannot reach the temperature threshold required for the formation of reedmergnerite, while the hydrothermal fluid becomes capable of providing the greatest possible chance of such a high temperature.
According to the phenomenon actually observed in the thin slices, it was found that reedmergnerite had a metasomatism relationship with alkaline minerals, such as sodium-calcium carbonate (Figure 4f), trona (Figure 4g), and carbonate minerals (Figure 3h and Figure 4a,b). Alkaline minerals and carbonate minerals have certain commonalities. Regarding chemical composition, alkaline minerals are carbonate minerals with different Na+ contents. Because the composition of carbonate minerals and alkaline minerals is different from that of reedmergnerite, two processes of dissolution and recrystallization were involved in the metasomatism [57]. Different dissolution degrees, different crystal habits, and different order degrees during recrystallization may be important reasons for the formation of different forms of reedmergnerite [49].
At present, there are different opinions on the division of the formation period of reedmergnerite, including the buried diagenetic period and quasi-contemporaneous period [24,39,46,56,63]. Temperature and pressure are the key factors in the formation of reedmergnerite [63]. The burial was shallow in the quasi-contemporaneous period. The temperature and pressure were not up to the formation conditions of reedmergnerite, and the carbonate minerals and alkaline minerals metasomatized by reedmergnerite were mainly developed in the Feng 2 Member, with a burial depth greater than 3000 m [56]. Therefore, it was speculated that the reedmergnerite was mainly formed by the metasomatism of carbonate minerals and alkaline minerals formed earlier under the action of an abnormal hydrothermal factor during burial diagenesis.

5.2. Diagenetic Evolutionary Sequence of Fengcheng Formation Shale Series in Mahu Sag

Characterized by the vitrinite reflectance (Ro) of mudstone in the Fengcheng Formation and supported by inclusion temperature, most reservoirs in the Fengcheng Formation are in middle diagenetic stage A, and a small part of them enter middle diagenetic stage B [68,69].

5.2.1. Devitrification and Hydrolysis

Volcanic glass material is unstable and often altered or devitrified to form stable clay minerals and zeolite under the action of volcanic activities and tectonic movements. The Fengcheng Formation contains a large amount of volcanic vitreous originally, which is widely distributed in clastic rock debris and volcanic rock matrix. Influenced by the environment, it can release a large amount of K+, Na+, Ca2+, Mg2+, and saline and alkaline interlayer pore water.

5.2.2. Diagenetic Mineral Precipitation Sequence

The first mineral to emerge from the solution was montmorillonite [70]. In the Fengcheng Formation, this part of montmorillonite was gradually transformed to form the Aemon mixed layer. With the further reaction, the salinity and alkalinity of the interlayer solution rose to the range of feldspar precipitation, and the feldspar precipitated was associated with clay minerals, followed by zeolite and quartz precipitation. The early zeolite was unstable, and with a further increase in temperature, it further generated zeolite and feldspar and released calcium ions, and the surplus calcium ions promoted the formation of calcite [61,71]. Under the conditions of temperature and pressure, and the abundant magnesium and iron ions in the solution, part of the montmorillonite was transformed into chlorite. Along with the hydrolytic alteration of volcanic glass materials, magnesite minerals, such as pyroxene, hornblende, biotite, and feldspar phenocrysts, crystal chips, and potassium feldspar in pyroclastic materials also have some chlorite (Figure 8). At the same time, the authigenic minerals precipitated under such environmental conditions are as follows: (1) bicarbonate minerals (carbonaceous calcium stone, trona, carbonaceous sodium magnesite, etc.); (2) salt minerals (sodium silicate, salt, etc.); (3) aluminum silicate minerals (potassium feldspar, albite, zeolite, etc.); (4) calcium and magnesium carbonate minerals (dolomite, calcite, etc.); (5) siliceous minerals (quartz, opal, etc.) [72].
The alteration process of the Fengcheng Formation can be classified as follows: (1) hydrolysis of volcanic glass, generation of montmorillonite, generation of zeolite minerals and related transformation, albitization; (2) chlorite influenced by magnesium and iron ions; (3) feldspar alteration, formation of chlorite and calcite, rest albite. In particular, hydrolysis occurred in the early diagenetic A stage. Dolomite formation can be divided into three stages, most of which were in early diagenetic stage B. Salt minerals were formed in the same generation. There are three phases of dissolution, which are scattered from the late early diagenetic stage to the middle diagenetic stage B (Figure 8).

5.3. Alkaline Sedimentary Evolution and Diagenetic Model of Fengcheng Formation Shale Series in Mahu Sag

Based on core slices from wells FN1, FN14, AK-1, and MH7 in the Mahu sag, combined with the literature data, the sedimentary evolution and the diagenetic model of the Fengcheng Formation in the alkaline lake environment were established from the aspects of climate, provenance, diagenetic environment, and underground fluids (Figure 9), which can be roughly divided into four stages: before the deposition of the Fengcheng Formation, during the deposition of the Fengcheng Formation, the low-temperature alkaline burial diagenetic stage, and the hydrothermal-related medium-high-temperature alkaline diagenetic stage.
Before the deposition of the Fengcheng Formation, in the arid/semi-arid climate, the lake water was evaporated and concentrated [41], resulting in a gradual increase in the alkalinity of the water body [57,62,63]. In addition, due to active volcanic activity, a large number of volcanic rocks developed at the bottom of the lake basin, and the low-temperature unstable minerals contained in the volcanic rocks were hydrolyzed, which provided Na+, Ca2+, Mg2+, and Fe2+ for the water body, which laid the material foundation for diagenesis and alkaline lake formation (Figure 9a).
During the deposition of the Fengcheng Formation, there were Cl−, CO32−, SO42−, and other anions in the lake basin. During the process of lake basin shrinkage and alkalization, the concentration of ions gradually increased, collided, and combined with each other, and a large number of Mg-Ca carbonate minerals and alkaline minerals with anions of CO32− appeared. In the presence of Mg2+, Na+, and Ca2+ plasmas, the order of binding with HCO3− and CO32− is Ca2+, Mg2+, and Na+ [73], with CaCO3 precipitation before MgCO3. After calcite precipitation, the lake water was stratified under the action of evaporation and concentration, which promoted the development of argillaceous sediments rich in organic matter [28]. The different types of organic matter were mainly from that organic matter [74,75], and their decay products were conducive to the large-scale development of carbonate minerals, forming lamellar carbonate mineral layers (mainly calcite) and argillaceous sediment layers. At this time, due to the large consumption of Ca2+, the Mg2+/Ca2+ ratio in the water body increased, and the Fe2+ was contributed by the volcanic tuff material. The microcrystal dolomite was also deposited [76]. The extensive development of carbonate minerals consumed a large amount of Ca2+ and Mg2+, while the content of Na+ increased relatively, and the consumed CO32− was continuously supplemented by volcanic activity.
With the further shrinkage of the lake basin water body, alkalinity reached the maximum amount, Na+ and CO32− tended to be saturated, and Na+ containing alkaline minerals such as trona and sodium-calcium carbonate was formed successively. Finally, the climate became hot and humid, and the water level rose. Under the supply of terrigenous detrital materials, materials such as mud and sand were deposited, and the sedimentary strata of the Fengcheng Formation were deposited (Figure 9b).
In the low-temperature alkaline diagenetic stage, the residual marine brine in the Carboniferous and Jiamuhe Formations underlying the Fengcheng Formation from the mid-Permian to the mid-Jurassic period [67], entering into the pores and fractures of the Fengcheng Formation along the fault under tectonic compression, it brought abundant elements such as Fe, Mn, and Mg [73] and cemented around the early calcite or calcite with a low degree of dolomitization, and the local distribution of fine-grained iron dolomite with clear ring was formed. With the surging of residual marine brine, Na+ was also present. In addition, the two necessary conditions of alkaline formation water and the rising temperature due to the formation’s burial were also present. The dissolution of quartz occurred, and the “salt effect” of Mg2+, K+, and Ca2+ in formation water further promoted the dissolution of quartz [52]. In this stage, in addition to the formation of iron dolomite and quartz dissolution, the cementation of laumontite also occurred under the background of alkaline diagenesis, low temperature, and the supply of Mg2+ and Fe2+ (Figure 9c).
The hydrocarbon source rocks of the Fengcheng Formation did not enter the oil generation threshold until the end of the Permian period [77], and kerogen began to transform into oil and gas. This process was accompanied by the formation of oxalic acid and acetic acid [13], where local pore fluid pH dropped and became acidic, resulting in the dissolution of early turbidite, iron dolomite, and alkaline minerals. The acidic fluid generated by oil and gas was neutralized by alkaline formation water and alkaline minerals, and the whole presented an alkaline diagenetic environment. During the middle-high-temperature alkaline diagenesis stage, the hydrothermal activity was intense at the end of the Triassic period [64], and the B-rich hydrothermal fluid migrated and upwelled along the fault. Reedmergnerite was formed by alkaline minerals containing Na+. Correspondingly, the mineral assemblages of reedmergnerite + calcite + iron dolomite, reedmergnerite + shortite, and reedmergnerite + mineral assemblages of trona can be found in the parts with incomplete metasomatism. Under the influence of the intercalated horizon of the fault, the distribution and morphology of the metasomatic minerals, and other factors, banded and agglomerated reedmergnerite was formed. As the overlying material continued to deposit, the burial depth increased. When the stone was enriched to a certain extent, it formed reedmergnerite-rich rocks (Figure 9d). Marked by the appearance of reedmergnerite, medium-high-temperature alkaline diagenesis occurred in the center and slope of the Mahu sag and near the fault zone, connecting the deep fluid and alkaline mineral layer and the carbonate layer [56].

6. Conclusions

In this paper, the types of shale series developed in the Fengcheng Formation in the Mahu sag include carbonate rocks, terrigenous detrital rocks, and alkaline mesobasic volcanic rocks, and there are bands and agglomerates rich in reedmergnerite. Under the combined influence of the supply of sodium-rich sources, an alkaline lake characterized by the development of alkaline minerals was formed, and experienced alkaline deposition and diagenesis was formed in an alkaline environment.
There were three types of diagenetic mineral assemblages and two types of alkaline diagenesis developed in the shale series of the Fengcheng Formation. The three mineral combinations include: carbonate mineral combination (calcite + iron dolomite), reedmergnerite and carbonate mineral combination (reedmergnerite + calcite + iron dolomite), and reedmergnerite and alkaline minerals combination (reedmergnerite + shortite + trona). According to the diagenetic temperature, the alkaline diagenesis of the Fengcheng Formation can be divided into two types: low-temperature alkaline burial diagenesis and medium-high-temperature alkaline diagenesis. The former is characterized by the formation of iron dolomite rings, quartz dissolution, and laumontite cementation, while the latter is characterized by the abundant presence of reedmergnerite.
Under the promotion of a long-term arid/semi-arid climate, based on underground fluids (hydrothermal and brine) and alkaline medium-basic volcanic parent rocks (substances) as the main material sources, in the special alkaline diagenetic environment of alkali lake, the alkaline sedimentary evolution–diagenetic model of the Fengcheng Formation, which was affected by climate, provenance, diagenetic environment, and underground fluid, was established. The model was divided into four stages: before the deposition of the Fengcheng Formation, sedimentary, low-temperature alkaline burial diagenesis, and hydrothermally related medium-high-temperature alkaline diagenesis.

Author Contributions

Conceptualization, methodology, and writing, B.B., J.L. and C.D.; review and editing, W.H. and C.D.; validation, Y.B. and X.C.; analysis and investigation, M.Z. and H.L.; supervision and editing, H.Z. All authors have read and agreed to the published version of the manuscript.

Funding

National Natural Science Foundation of China (No. 42090025, 42072186), Petrochina Co., Ltd. Technology Support Program (2022DQ0525, 2021–DJ2203).

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

Data are contained within the article.

Acknowledgments

The authors express their gratitude to Zhenkun Yu for support and assistance during the field visit and data collection.

Conflicts of Interest

Authors Bin Bai, Wenjun He and Ying Bai were employed by the company PetroChina. The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest. The authors declare that this study received funding from Petrochina Co., Ltd. The funder was not involved in the study design, collection, analysis, interpretation of data, the writing of this article or the decision to submit it for publication.

Abbreviations

The following abbreviations are used in this manuscript:
EPMAelectron probe microanalysis
SEMscanning electron microscope
CLcathode luminescence
LRlaser Raman
Calcalcite
Fer-DOLferric dolomite
Rdreedmergnerite
TroTrone
Stshortite
Lmtlaumontite cemented between particles

References

  1. Kuang, L.C.; Tang, Y.; Lei, D.W.; Chang, Q.S.; Ouyang, M.; Hou, L.H.; Liu, D.G. Formation conditions and exploration potential of tight oil in the Permian saline lacustrine dolomitic rock, Junggar Basin, NW China. Pet. Explor. Dev. 2012, 39, 657–667. [Google Scholar] [CrossRef]
  2. Kuang, L.C.; Cui, X.K.; Zou, C.N.; Hou, L.H. Oil accumulation and concentration regularity of volcanic lithostratigraphic oil reservoir: A case from upper-plate Carboniferous of KA-BAI fracture zone, Junggar Basin. Pet. Explor. Dev. 2007, 34, 285–290. [Google Scholar]
  3. Yu, K.; Cao, Y.; Qiu, L.; Sun, P. The hydrocarbon generation potential and migration in an alkaline evaporate basin: The Early Permian Fengcheng Formation in the Junggar Basin, northwestern China. Mar. Pet. Geol. 2018, 98, 12–32. [Google Scholar] [CrossRef]
  4. Jagniecki, E.A.; Jenkins, D.M.; Lowenstein, T.K.; Carroll, A.R. Experimental Study of Shortite (Na2Ca2(CO3)3) Formation and Application to the Burial History of the Wilkins Peak Member, Green River Basin, Wyoming, USA. Geochim. Cosmochim. Acta 2013, 115, 31–45. [Google Scholar] [CrossRef]
  5. Smith, M.E.; Carroll, A.R.; Singe, B.S. Synoptic Reconstruction of a Major Ancient Lake System: Eocene Green River Formation, Western United States. Geol. Soc. Am. Bull. 2008, 120, 54–84. [Google Scholar] [CrossRef]
  6. Javier, G.V.; Ibrahim, G.; Cahit, H.; Eva, P. Genetic Model for Na-Carbonate Mineral Precipitation in the Miocene Beypazarı Trona Deposit, Ankara Province, Turkey. Sediment. Geol. 2013, 294, 315–327. [Google Scholar]
  7. Meng, T.; Liu, P.; Qiu, L.W.; Wang, Y.S.; Liu, Y.L.; Lin, H.M.; Cheng, F.Q.; Qu, C.S. Formation and distribution of the high quality reservoirs in a deep saline lacustrine basin: A case study from the upper part of the 4th member of Paleogene Shahejie Formation in Bonan sag, Jiyang depression, Bohai Bay Basin, East China. Pet. Explor. Dev. 2017, 44, 896–906. [Google Scholar] [CrossRef]
  8. Tang, Y.; Lyu, Z.X.; He, W.J.; Qing, Y.H.; Li, X.; Song, X.Z.; Yang, S.; Cao, Q.M.; Qian, Y.X.; Zhao, X.M. Origin of dolomites in the Permian dolomitic reservoirs of Fengcheng Formation in Mahu Sag, Junggar Basin, NW China. Pet. Explor. Dev. 2023, 50, 38–50. [Google Scholar] [CrossRef]
  9. Jiang, F.J.; Hu, M.L.; Hu, T.; Lyu, J.H.; Huang, L.L.; Liu, C.L.; Jiang, Z.X.; Huang, R.D.; Zhang, C.X.; Wu, G.Y.; et al. Controlling factors and models of shale oil enrichment in Lower Permian Fengcheng Formation, Mahu Sag, Junggar Basin, NW China. Pet. Explor. Dev. 2023, 50, 706–718. [Google Scholar] [CrossRef]
  10. Tang, Y.; Cao, J.; He, W.J.; Guo, X.G.; Zhao, K.B.; Li, W.W. Discovery of shale oil in alkaline lacustrine basins: The Late Paleozoic Fengcheng Formation, Mahu Sag, Junggar Basin, China. Pet. Sci. 2021, 18, 1281–1293. [Google Scholar] [CrossRef]
  11. Qiu, L.W.; Jang, Z.X.; Cao, Y.C.; Qiu, R.H.; CHEN, W.X.; TU, Y.F. Alkaline diagenesis and its influence on a reservoir in the Biyang depression. Sci. China Ser. D 2002, 45, 643–653. [Google Scholar] [CrossRef]
  12. Li, S.Y.; Tian, J.C.; Lin, X.B.; Zuo, Y.H.; Kang, H.; Yang, D.D. Effect of alkaline diagenesis on sandstone reservoir quality: Insights from the Lower Cretaceous Erlian Basin, China. Energy Explor. Exploit. 2002, 38, 434–453. [Google Scholar] [CrossRef]
  13. Zhang, S.B.; Liu, Z.; Liu, H.J.; Song, Y.H.; Li, X.M.; Xu, T. Alkali Diagenesis of Xujiahe Sandstone in Hebaochang Block in Sichuan Basin. Xingjiang Pet. Geol. 2011, 32, 464–468. [Google Scholar]
  14. Cao, T.Y.; Zhong, D.K.; Niu, S.L.; Sun, H.T.; Cao, X.; Wang, F. Alkaline Diagenesis and Porosity Evolution of Zhu hai Formation Reservoirs in Eastern Huizhou Sag. Acta Sedimentol. Sin. 2020, 38, 1327–1337. [Google Scholar]
  15. Zhu, H.H.; Zhong, D.K.; Yao, J.L.; Sun, H.T.; Niu, X.B.; Liang, X.W.; You, Y.; Li, X. Alkaline diagenecs and its effects on reservoir porosity: A case study of Upper Triassic Chang 7 Member tight sandstone in Ordos Basin, NW China. Pet. Explor. Dev. 2015, 42, 56–65. [Google Scholar] [CrossRef]
  16. Hu, T.; Pang, X.Q.; Jiang, S.; Wang, Q.F.; Xu, T.W.; Lu, K.; Huang, C.; Chen, Y.Y.; Zheng, X.W. Impact of Paleosalinity, Dilution, Redox, and Paleoproductivity on Organic Matter Enrichment in a Saline Lacustrine Rift Basin: A Case Study of Paleogene Organic-Rich Shale in Dongpu Depression, Bohai Bay Basin, Eastern China. Energy Fuels 2008, 32, 5045–5061. [Google Scholar] [CrossRef]
  17. Chen, Z.Y.; Chen, J.F.; Zhong, N.N.; Fei, W.W.; Dong, Q.W.; Chen, J.; Wang, Y.Y. The geneses of sedimentary organic matter with anomalous 13C-enriched isotopic composition in saline and freshwater lakes: A case study of lacustrine source rocks from Dongpu and Qikou sags, Bohai Bay Basin, eastern China. Mar. Pet. Geol. 2020, 118, 104434. [Google Scholar] [CrossRef]
  18. Wang, K.; Pang, X.Q.; Zhang, H.G.; Zhao, Z.F.; Su, S.C.; Hui, S.S. Characteristics and genetic types of natural gas in the northern Dongpu Depression, Bohai Bay Basin, China. J. Pet. Sci. Eng. 2018, 170, 453–466. [Google Scholar] [CrossRef]
  19. Tan, X.F.; Tian, J.C.; Li, Z.B.; Zhang, S.P.; Wang, W.Q. Diagenesis evolution of fragmental reservoir in alkali sediment environment-taking the Member 4 of Shahejie Formation of steep-slope zone in Dongying sag, Shandong, China for example. Geol. Bull. China 2010, 4, 535–543. [Google Scholar]
  20. Tang, W.B.; Zhang, Y.Y.; Georgia, P.P.; David, J.W.P.; Guo, Z.J.; Li, W. Permian to early Triassic tectono-sedimentary evolution of the Mahu sag, Junggar Basin, western China: Sedimentological implications of the transition from rifting to tectonic inversion. Mar. Pet. Geol. 2021, 123, 104730. [Google Scholar] [CrossRef]
  21. He, D.F.; Li, D.; Fan, C.; Yang, X.F. Geochronology, geochemistry and tectonostratigraphy of Carboniferous strata of the deepest Well Moshen-1 in the Junggar Basin, northwest China: Insights into the continental growth of Central Asia. Gondwana Res. 2013, 24, 560–577. [Google Scholar] [CrossRef]
  22. Cao, J.; Lei, D.; Li, Y.; Tang, Y.; Chang, Q.; Abulimit, I.; Wang, T. Ancient high-quality alkaline lacustrine source rocks discovered in the Lower Permian Fengcheng Formation, Junggar Basin. Acta Pet. Sin. 2015, 36, 781–790. [Google Scholar] [CrossRef]
  23. Cao, J.; Xia, L.W.; Wang, T.T.; Zhi, D.M. An alkaline lake in the Late Paleozoic Ice Age (LPIA): A review and new insights into paleoenvironment and petroleum geology. Earth-Sci. Rev. 2020, 202, 103091. [Google Scholar] [CrossRef]
  24. Zhang, Z.J.; Yuan, X.J.; Wang, M.S.; Zhou, C.M.; Tang, Y.; Chen, X.Y.; Lin, M.J.; Cheng, D.W. Alkaline-lacustrine deposition and paleoenvironmental evolution in permian fengcheng formation at the mahu sag, junggar basin, nw china. Pet. Explor. Dev. 2018, 45, 1036–1049. [Google Scholar] [CrossRef]
  25. Yu, K.H.; Cao, Y.C.; Qiu, L.W.; Sun, P.P.; Jia, X.Y.; Wan, M. Geochemical characteristics and origin of sodium carbonates in a closed alkaline basin: The Lower Permian Fengcheng Formation in the Mahu Sag, northwestern Junggar Basin, China. Palaeogeogr. Palaeoclimatol. Palaeoecol. 2018, 511, 506–531. [Google Scholar] [CrossRef]
  26. He, D.F.; Yin, C.; Du, S.K.; Shi, X.; Ma, H.S. Characteristics of structural segmentation of foreland thrust belts -A case study of the fault belts in the northwestern margin of Junggar Basin. Earth Sci. Front. 2004, 3, 91–101. [Google Scholar]
  27. Li, D.; He, D.F.; Santosh, M.; Ma, D.L.; Tang, J.Y. Tectonic framework of the northern Junggar Basin part I: The eastern Luliang Uplift and its link with the East Junggar terrane. Gondwana Res. 2015, 27, 1089–1109. [Google Scholar] [CrossRef]
  28. Cao, J.; Yao, S.P.; Jin, Z.J.; Hu, W.X.; Zhang, Y.J.; Wang, X.L.; Zhang, Y.Q.; Tang, Y. Petroleum migration and mixing in the northwestern Junggar Basin (NW China): Constraints from oil-bearing fluid inclusion analyses. Org. Geochem. 2006, 37, 827–846. [Google Scholar] [CrossRef]
  29. Xu, Z.H.; Hu, S.Y.; Wang, L.; Zhao, W.Z.; Cao, Z.L.; Wang, R.J.; Shi, S.Y.; Jiang, L. Seismic sedimentologic study of facies and reservoir in middle Triassic Karamay Formation of the Mahu Sag, Junggar Basin, China. Mar. Pet. Geol. 2019, 107, 222–236. [Google Scholar] [CrossRef]
  30. Chen, Z.L.; Liu, G.D.; Wang, X.L.; Gao, G.; Xiang, B.L.; Ren, J.L.; Ma, W.Y.; Zhang, Q. Origin and mixing of crude oils in Triassic reservoirs of Mahu slope area in Junggar Basin, NW China: Implication for control on oil distribution in basin having multiple source rocks. Mar. Pet. Geol. 2016, 78, 373–389. [Google Scholar] [CrossRef]
  31. Liang, Y.Y.; Zhang, Y.Y.; Chen, S.; Guo, Z.J.; Tang, W.B. Controls of a strike-slip fault system on the tectonic inversion of the Mahu depression at the northwestern margin of the Junggar Basin, NW China. J. Asian Earth Sci. 2020, 198, 104229. [Google Scholar] [CrossRef]
  32. Lei, D.; Chen, G.; Liu, H.; Li, X.; Abulimit, T.K.; Cao, J. Study on the forming conditions and exploration fields of the Mahu Giant Oil (Gas) Province, Junggar Basin. Acta Geol. Sin. 2017, 91, 1604–1619. [Google Scholar]
  33. Zhang, G.Y.; Wang, Z.Z.; Guo, X.G.; Sun, Y.Y.; Sun, L.; Pan, L. Characteristics of lacustrine dolomitic rock reservoir and accumulation of tight oil in the Permian Fengcheng Formation, the western slope of the Mahu Sag, Junggar Basin, NW China. J. Asian Earth Sci. 2019, 178, 64–80. [Google Scholar] [CrossRef]
  34. Chen, Y.B.; Cheng, X.G.; Zhang, H.; Li, C.Y.; Ma, Y.P.; Wang, G.D. Fault characteristics and control on hydrocarbon accumulation of middle-shallow layers in the slope zone of Mahu sag, Junggar Basin, NW China. Pet. Explor. Dev. 2018, 6, 1050–1060. [Google Scholar] [CrossRef]
  35. Feng, C.; Li, T.; He, W.J.; Zheng, M.L. Organic geochemical traits and paleo-depositional conditions of source rocks from the Carboniferous to Permian sediments of the northern Mahu Sag, Junggar Basin, China. J. Pet. Sci. Eng. 2020, 191, 107117. [Google Scholar] [CrossRef]
  36. Li, J.; Tang, Y.; Wu, T.; Zhao, J.Z.; Wu, H.Y.; Wu, W.T.; Bai, Y.B. Overpressure origin and its effects on petroleum accumulation in the conglomerate oil province in Mahu Sag, Junggar Basin, NW China. Pet. Explor. Dev. 2020, 47, 726–739. [Google Scholar] [CrossRef]
  37. Yang, M.Z.; Wang, F.Z.; Zheng, J.P. Geochemistry and tectonic setting of basic volcanic rocks in Ke-Xia region, northwestern Junggar Basin. Acta Petrol. Miner. 2006, 20, 165–174. [Google Scholar]
  38. Wu, W.; Li, Q.; Pei, J.X.; Ning, S.Y.; Tong, L.Q.; Liu, W.Q.; Feng, Z.D. Seismic sedimentology, facies analyses, and high-quality reservoir predictions in fan deltas: A case study of the Triassic Baikouquan Formation on the western slope of the Mahu Sag in China’s Junggar Basin. Mar. Pet. Geol. 2020, 120, 104546. [Google Scholar] [CrossRef]
  39. Wang, M.S.; Zhang, Z.J.; Zhou, C.M.; Yuan, X.J.; Lin, M.J.; Liu, Y.H.; Cheng, D.W. Lithological characteristics and origin of alkaline lacustrine of the Lower Permian Fengcheng Formation in Mahu Sag, Junggar Basin. J. Paleogeogr. 2018, 20, 147–162. [Google Scholar]
  40. Xu, L.; Chang, Q.S.; Feng, L.L.; Zhang, N.; Liu, H. The reservoir characteristics and control factors of shale oil in Permian Fengcheng Formation of Mahu sag, Junggar Basin. China Pet. Explor. 2019, 24, 649–660. [Google Scholar]
  41. Yu, K.H.; Cao, Y.C.; Qiu, L.W.; Sun, P.; Yang, Y.Q.; Qu, C.S.; Wan, M. Characteristics of alkaline layer cycles and origin of the Lower Permian Fengcheng Formation in Mahu sag, Junggar Basin. J. Paleogeogr. 2016, 18, 1012–1029. [Google Scholar]
  42. You, X.L.; Jia, W.Q.; Xu, F.; Liu, Y. Mineralogical characteristics of ankerite and mechanisms of primary and secondary origins. Earth Sci. 2018, 43, 4046–4055. [Google Scholar]
  43. Pagel, M.; Barbin, V.; Blanc, P.; Ohnenstetter, D. Application of Cathodoluminescence to Carbonate Diagenesis, 1st ed.; Springer: Berlin, Germary, 2000; pp. 271–301. [Google Scholar]
  44. Axel, G.; Detlev, K.R.; Jan, M.; Rolf, D.N.; Andreas, S. Quantitative high resolution cathodoluminescence spectroscopy of diagenetic and hydrothermal dolomites. Sediment. Geol. 2001, 140, 191–199. [Google Scholar]
  45. Braith, J.R. Cathodoluminescence in Quaternary caibonate deposits. Sediment. Geol. 2016, 337, 29–35. [Google Scholar] [CrossRef]
  46. Goldstein, H.R. Systematics of fluid inclusions in diagenetic minerals. SEPM Short Course 1994, 31, 199. [Google Scholar]
  47. Eugster, H.P.; Mciver, N.L. Boron analogues of alkali feldspars and related silicates. Bull. Geol. Soc. Am. 1959, 70, 1598. [Google Scholar]
  48. Hou, L.H.; Zou, C.N.; Liu, L.; Wen, B.H.; Wu, X.Z.; Wei, Y.Z.; Mao, Z.G. Geologic essential elements for hydrocarbon accumulation with in Carboniferous volcanic weathered crusts in Xinjiang, China. Acta Pet. Sin. 2012, 33, 533–540. [Google Scholar]
  49. Xue, J.J.; Sun, J.; Zhu, X.M.; Liu, W.; Zhu, S.F. Characteristics and Formation Mechanism for Dolomite Reservoir of Permian Fengcheng Formation in Junggar Basin. Geoscience 2012, 26, 755–761. [Google Scholar]
  50. Qiu, L.W.; Jiang, Z.X.; Chen, W.X. A new type of secondary porosity--quartz dissolution porosity. Acta Sedimentol. Sin. 2002, 4, 621–627. [Google Scholar]
  51. Qu, X.Y.; Chen, X.; Qiu, L.W.; Zhang, M.L.; Zhang, X.J. Genesis of secondary pore of quartz dissolution type and its influences on reservoir: Taking the tight sandstone reservoir in the Upper Paleozoic of Daniudi gas field as an example. Oil Gas Geol. 2015, 36, 804–813. [Google Scholar]
  52. Liu, J.K.; Peng, J.; Shi, Y.; Bao, Z.F.; Sun, Y.L.; Liu, X.M.; Zhang, Z. The genesis of quartz dissolution in tight sand reservoirs and its impact on pore development: A case study of Xujiahe Formation in the transitional zone of Central-Southern Basin. Acta Pet. Sin. 2015, 36, 1090–1097. [Google Scholar]
  53. Rimstidt, J.D.; Zhang, Y.L.; Zhu, C. Rate equations for sodium catalyzed amorphous silica dissolution. Geochim. Cosmochim. Acta 2016, 195, 120–125. [Google Scholar] [CrossRef]
  54. Zhang, S.T.; Liu, Y. Molecular-level mechanisms of quartz dissolution under neutral and alkaline conditions in the presence of electrolytes. Geochem. J. 2014, 48, 189–205. [Google Scholar] [CrossRef]
  55. Yu, K.H.; Cao, Y.C.; Qiu, L.W.; Sun, P.P.; Su, Y.G. Brine evolution of ancient lake and mechanism of carbonate minerals during the sedimentation of Early Permian Fengcheng Formation in Mahu Depression, Junggar Basin, China. Nat. Gas Geosci. 2016, 27, 1248–1263. [Google Scholar]
  56. Zhao, Y.; Guo, P.; Lu, Z.Y.; Zheng, R.C.; Chang, H.L.; Wang, G.Z.; Wei, Y.; Wen, H.G. Genesis of Reedmergnerite in the Lower Permian Fengcheng Formation of the Junggar Basin, NE China. Acta Sedimentol. Sin. 2020, 38, 966–979. [Google Scholar]
  57. Zhang, H.; Cheng, L.; Fan, H.T. Formation overpressure and its influence on physical properties in Mahu sag, Junggar Basin. Prog. Geophys. 2022, 37, 1223–1227. [Google Scholar]
  58. Zhang, S.T.; Liu, Y. Progress Review of Quartz Dissolution Models. Bull. Miner. Petrol. Geochem. 2009, 28, 294–300. [Google Scholar]
  59. Tian, X.R.; Zhang, Y.Y.; Zhuo, Q.G.; Yu, Z.C.; Guo, Z.J. Tight oil charging characteristics of the Lower Permian Fengcheng Formation in Mahu sag, Junggar Basin: Evidence from fluid in alkaline minerals. Acta Pet. Sin. 2019, 40, 646–659. [Google Scholar]
  60. Rao, S.; Zhu, Y.K.; Hu, S.B.; Wang, Q. The Thermal History of Junggar Basin: Constraints on the Tectonic Attribute of the Early-Middle Permian Basin. Acta Geol. Sin. 2018, 92, 1176–1195. [Google Scholar]
  61. Zhu, S.F.; Zhu, X.M.; Wu, D.; Liu, Y.H.; Li, P.P.; Jiang, S.X.; Liu, X.C. Alteration of volcanics and its controlling factors in the Lower Permian reservoirs at northwestern margin of Junggar Basin. Oil Gas Geol. 2014, 35, 77–85. [Google Scholar]
  62. Guo, M.Z.; Shou, J.F.; Xu, Y.; Guo, H.J.; Zou, Z.W.; Han, S.H. Distribution and controlling factors of Permian zeolite cements in Zhongguai—Northwest margin of Junggar Basin. Acta Pet. Sin. 2016, 37, 695–705. [Google Scholar]
  63. Chipera, S.J.; Goff, F.; Goff, C.J.; Fittipaldo, M. Zeolitization of intracaldera sediments and rhyolitic rocks in the 1.25 Ma lake of Valles caldera, New Mexico, USA. J. Volcanol. Geotherm. Res. 2008, 178, 317–330. [Google Scholar] [CrossRef]
  64. Zhu, S.F.; Zhu, X.M.; Liu, X.C.; Li, C.; Wang, X.X.; Tan, M.X.; Geng, M.Y.; Li, Y.P. Alteration products of volcanic materials and their influence on reservoir space in hydrocarbon reservoirs: Evidence from Lower Permian strata in Ke-Xia region, Junggar Basin. Acta Pet. Sin. 2014, 35, 276–285. [Google Scholar]
  65. Zhu, S.F.; Zhu, X.M.; Wang, X.L.; Liu, Z.Y. Zeolite diagenesis and its control on petroleum reservoir quality of Permian in northwestern margin of Junggar Basin, China. Sci. China Earth Sci. 2012, 55, 386–396. [Google Scholar] [CrossRef]
  66. Chang, H.L.; Zheng, R.C.; Guo, C.L.; Wen, H.G. Characteristics of Rare Earth Elements of Exhalative Rock in Fengcheng Formation, Northwestern Margin of Jungger Basin. Geol. Rev. 2016, 62, 550–568. [Google Scholar]
  67. Zhu, S.F.; Zhu, X.M.; Niu, H.P.; Han, X.F.; Zhang, Y.Q. Genetic Mechanism of Dolomitization in Fengcheng Formation in the Wu-Xia area of Junggar Basin, China. Acta Geol. Sin.-Engl. Ed. 2012, 86, 447–461. [Google Scholar]
  68. Guo, P.; Wen, H.G.; Gibert, L.; Jin, J.; Jiang, Y.Q.; Wang, G.Z. Controlling factors of high quality hydrocarbon source rocks developed in lacustrine shallow-water zone of the Junggar Basin, northwestern China. AAPG Bull. 2021, 105, 2063–2092. [Google Scholar] [CrossRef]
  69. Guo, P.; Wen, H.; Gibert, L.; Jin, J.; Wang, J.; Lei, H. Deposition and diagenesis of the Early Permian volcanic-related alkaline playa-lake dolomitic shales, NW Junggar Basin, NW China. Mar. Pet. Geol. 2020, 123, 104780. [Google Scholar] [CrossRef]
  70. Broxton, D.E. Chemical changes associated with zeolitization of the tuffaceous beds of Calico Hills, Yucca Mountain, Nevada, USA. Proc. Int. Symp. Water-Rock Interact. 1992, 7, 699–703. [Google Scholar]
  71. Lijima, A. Zeolites in petroleum and natural gas reservoirs. Rev. Mineral. Geochem. 2001, 45, 347–402. [Google Scholar]
  72. Jia, B.; Wen, H.G.; Li, Y.B.; Liu, Y.P.; Wang, T. Fluid inclusions in the salt minerals from the Permian Fengcheng Formation in the Urho region, Junggar Basin, Xinjiang. Sediment. Geol. Tethyan Geol. 2015, 35, 33–42. [Google Scholar]
  73. Lovley, D.R.; Holmes, D.E.; Nevin, K.P. Dissimilatory Fe(III) and Mn(IV) reduction. Adv. Microb. Physiol. 2004, 49, 219–286. [Google Scholar]
  74. Jin, Q.; Wang, J.; Song, G.Q.; Wang, L.; Lin, L.M.; Bai, S.P. Interaction between source rock and evaporite: A case study of natural gas generation in the northern dongying depression. Chin. J. Geochem. 2010, 29, 75–81. [Google Scholar] [CrossRef]
  75. Zhi, D.M.; Tang, Y.; Zheng, M.L.; Xu, Y.; Cao, J.; Ding, J.; Zhao, C.Y. Geological characteristics and accumulation controlling factors of shale reservoirs in Fengcheng Formation, Mahu sag, Junggar Basin. China Pet. Explor. 2019, 24, 615–623. [Google Scholar]
  76. Hips, K.; Haas, J.; Poros, Z.; Kele, S.; Budai, T. Dolomitization of Triassic microbial mat deposits (Hungary): Origin of microcrystalline dolomite. Sediment. Geol. 2015, 318, 113–129. [Google Scholar] [CrossRef]
  77. Cao, J.; Zhang, Y.J.; Hu, W.X.; Yao, S.P.; Wang, X.L.; Zhang, Y.Q.; Tang, Y. The Permian hybrid petroleum system in the northwest margin of the Junggar Basin, northwest China. Mar. Pet. Geol. 2005, 22, 331–349. [Google Scholar] [CrossRef]
Applsci 13 13186 g001
Figure 1. Tectonic and lithofacies paleogeographic maps of the Mahu Depression in the Junggar Basin: (a) map of tectonic units in the Mahu Depression, Junggar Basin (with well location) (adapted from [14,27]); (b) lithologic columns of the Permian and Fengcheng Formation in the Mahu Depression (adapted from [26]); (c) source-reservoir-cap assemblage diagram (taking well FN1 as an example).
Figure 1. Tectonic and lithofacies paleogeographic maps of the Mahu Depression in the Junggar Basin: (a) map of tectonic units in the Mahu Depression, Junggar Basin (with well location) (adapted from [14,27]); (b) lithologic columns of the Permian and Fengcheng Formation in the Mahu Depression (adapted from [26]); (c) source-reservoir-cap assemblage diagram (taking well FN1 as an example).
Applsci 13 13186 g001
Applsci 13 13186 g002
Figure 2. Petrological characteristics of volcanic rocks in the Mahu Depression. Subvolcanics: (a) basaltic porphyrite; (b) andesitic porphyrite and volcanic lava; (c) basal; (d) trachyte and volcanic clastic rocks; (e) tuff; (f) tuff breccia.
Figure 2. Petrological characteristics of volcanic rocks in the Mahu Depression. Subvolcanics: (a) basaltic porphyrite; (b) andesitic porphyrite and volcanic lava; (c) basal; (d) trachyte and volcanic clastic rocks; (e) tuff; (f) tuff breccia.
Applsci 13 13186 g002
Applsci 13 13186 g003
Figure 3. Petrological characteristics in the Mahu Depression, Junggar Basin: (a) MY1-F2, characteristics of lamellar iron dolomite under cathodoluminescence; (b,c) FN14-F2, microscopic characteristics of massive iron dolomite and its cathodoluminescence properties; (d,e) FN14-F2, microscopic characteristics of snowflake iron dolomite and its cathodoluminescence properties; (f) FN14-F2, bright iron-poor nuclei (Cal), the number of bands indicated by 1, 2, 3, 4, 5; (g) FN14-F2, the calcite (Cal) in the belt is metasomatized almost entirely by ferric dolomite (Fer-DOL), which is metasomatized later by reedmergnerite (Rd); (h) FN14-F2, skeletal crystalline reedmergnerite with irregular radial edges.
Figure 3. Petrological characteristics in the Mahu Depression, Junggar Basin: (a) MY1-F2, characteristics of lamellar iron dolomite under cathodoluminescence; (b,c) FN14-F2, microscopic characteristics of massive iron dolomite and its cathodoluminescence properties; (d,e) FN14-F2, microscopic characteristics of snowflake iron dolomite and its cathodoluminescence properties; (f) FN14-F2, bright iron-poor nuclei (Cal), the number of bands indicated by 1, 2, 3, 4, 5; (g) FN14-F2, the calcite (Cal) in the belt is metasomatized almost entirely by ferric dolomite (Fer-DOL), which is metasomatized later by reedmergnerite (Rd); (h) FN14-F2, skeletal crystalline reedmergnerite with irregular radial edges.
Applsci 13 13186 g003
Applsci 13 13186 g004
Figure 4. Alkaline diagenesis characteristics in the Mahu Depression, Junggar Basin: (a) FN14-F2, wedge-shaped reedmergnerite is clustered together, and some of it contains residual calcite (Cal); (b) FN14-F2, rhomboid reedmergnerite with serrated edges; (c) FN14-F2, under cathodoluminescence, the reedmergnerite shows dark blue; (d) FN14-F2, reedmergnerite (Rd) metasomatism of shortite (St) from the edge; (e) AK1-F2, reedmergnerite (Rd) is symbiotic with trona (Tro); (f) FN14-F1, the edge of quartz grain is corroded into a serrated or bay shape; (g) MY1-F1, the internal surface of quartz was dissolved to form a “honeycomb” pit, 200 times; (h) MY1-F1, laumontite cemented between particles (Lmt).
Figure 4. Alkaline diagenesis characteristics in the Mahu Depression, Junggar Basin: (a) FN14-F2, wedge-shaped reedmergnerite is clustered together, and some of it contains residual calcite (Cal); (b) FN14-F2, rhomboid reedmergnerite with serrated edges; (c) FN14-F2, under cathodoluminescence, the reedmergnerite shows dark blue; (d) FN14-F2, reedmergnerite (Rd) metasomatism of shortite (St) from the edge; (e) AK1-F2, reedmergnerite (Rd) is symbiotic with trona (Tro); (f) FN14-F1, the edge of quartz grain is corroded into a serrated or bay shape; (g) MY1-F1, the internal surface of quartz was dissolved to form a “honeycomb” pit, 200 times; (h) MY1-F1, laumontite cemented between particles (Lmt).
Applsci 13 13186 g004
Applsci 13 13186 g005
Figure 5. Laser Raman spectroscopy of reedmergnerite.
Figure 5. Laser Raman spectroscopy of reedmergnerite.
Applsci 13 13186 g005
Applsci 13 13186 g006
Figure 6. Fluid characteristics of the fluid inclusion in reedmergnerite. (a) FN2, reedmergnerite text. (b) FN2, Growth Zone (GZ) surrounded by fluid inclusions in reedmergnerite. (c) FN1, Cluster like distribution of fluid inclusions in reedmergnerite. (d) FN1, random distribution (RP) fluid inclusions in reedmergnerite. (e) FN3, long trail (LT) in cutting shortite crystals. (f) FN1, long trail (LT) in cutting reedmergnerite crystals. (g) FN1, long trail (LT) in cutting reedmergnerite crystals, gas liquid two-phase inclusions. (h) FN1, gas liquid two-phase inclusions. (i) FN1, long trail (LT) in cutting reedmergnerite crystals, liquid-dominated biphase-inclusisions(L-D).
Figure 6. Fluid characteristics of the fluid inclusion in reedmergnerite. (a) FN2, reedmergnerite text. (b) FN2, Growth Zone (GZ) surrounded by fluid inclusions in reedmergnerite. (c) FN1, Cluster like distribution of fluid inclusions in reedmergnerite. (d) FN1, random distribution (RP) fluid inclusions in reedmergnerite. (e) FN3, long trail (LT) in cutting shortite crystals. (f) FN1, long trail (LT) in cutting reedmergnerite crystals. (g) FN1, long trail (LT) in cutting reedmergnerite crystals, gas liquid two-phase inclusions. (h) FN1, gas liquid two-phase inclusions. (i) FN1, long trail (LT) in cutting reedmergnerite crystals, liquid-dominated biphase-inclusisions(L-D).
Applsci 13 13186 g006
Applsci 13 13186 g007
Figure 7. Homogenization temperature histogram of reedmergnerite primary fluid inclusions.
Figure 7. Homogenization temperature histogram of reedmergnerite primary fluid inclusions.
Applsci 13 13186 g007
Applsci 13 13186 g008
Figure 8. Sequence diagram of the diagenetic evolution of the Fengcheng Formation in Mahu sag.
Figure 8. Sequence diagram of the diagenetic evolution of the Fengcheng Formation in Mahu sag.
Applsci 13 13186 g008
Applsci 13 13186 g009
Figure 9. Alkaline sedimentary evolution–diagenesis model of the Fengcheng Formation (the faults shown are schematic faults [24,39]. (a) before the deposition of the Fengcheng Formation (b) during the sedimentation of the Fengcheng Formation. (c) low-temperature alkaline burial diagenesis. (d) medium-high-temperature alkaline diagenesis.
Figure 9. Alkaline sedimentary evolution–diagenesis model of the Fengcheng Formation (the faults shown are schematic faults [24,39]. (a) before the deposition of the Fengcheng Formation (b) during the sedimentation of the Fengcheng Formation. (c) low-temperature alkaline burial diagenesis. (d) medium-high-temperature alkaline diagenesis.
Applsci 13 13186 g009
Table 1. EPMA data table of titanaugite and iron dolomite (wt.%).
Table 1. EPMA data table of titanaugite and iron dolomite (wt.%).
Na2OTiO2SO3SiO2FeOP2O5Al2O3MnOK2OMgOBaOCaOTotal
Iron dolomite0.070.22--9.39-0.010.460.0115.490.0927.9153.65
---0.039.380.060.020.620.0215.01-27.8552.99
--0.06-8.01--0.110.0117.58-30.8456.61
----6.440.020.020.37-17.990.0932.0256.95
-0.040.040.0112.99-0.050.33-13.96-29.4556.87
--0.04-10.980.040.010.540.0113.740.0728.0353.46
---0.166.69-0.080.180.0317.850.0431.1056.13
--0.04-8.410.01-1.210.0418.25-32.0560.01
-0.05--7.450.01-0.86-17.490.1330.4656.45
0.070.080.258.545.430.081.860.160.5415.58-23.5856.17
Titanagite0.02420.2760.05637.5138.6870.0516.7450.1220.1162.2430.07318.15694.06
Table 2. EPMA data table of reedmergnerite (wt.%).
Table 2. EPMA data table of reedmergnerite (wt.%).
Na2OTiO2SO3SiO2FeOP2O5Al2O3MnOK2OMgOBaOCaOB2O5Total
10.000--70.517----0.0010.0100.025-19.447100
10.000-0.01069.7670.028- 0.0430.012 --20.11899.98
13.794--71.1650.0090.0250.047--0.007-0.00514.948100
11.9360.065-69.3770.0170.0170.068-0.0620.0140.0160.01318.415100
10.012-0.16269.6970.0200.0170.086-0.0880.027--19.891100
10.0000.258-70.632--0.0940.0090.0080.0280.007-18.964100
10.0630.0800.03170.288--0.010-0.015---19.513100
10.042-0.00570.0150.004-0.0030.0250.024--0.00419.878100
10.0720.032-64.8680.0090.0170.0040.0240.0210.018--20.93596
Table 3. Results of homogenization temperature of the fluid inclusion in reedmergnerite.
Table 3. Results of homogenization temperature of the fluid inclusion in reedmergnerite.
BoreholeDeep/mFluid Inclusions OccurrenceAssociations of Fluid InclusionsTypeSize/μmHomogenization Temperature/°C
Fengnan24100.58growth zoneFIA-1gas and liquid20112
liquid10100
liquid15111
Fengnan24100.58growth zoneFIA-2gas and liquid5112
gas and liquid4100
liquid4111
liquid5112
liquid4100
Fengnan24100.58growth zoneFIA-3gas and liquid4111
gas and liquid6104
gas and liquid5103
liquid7109
liquid5110
liquid7116
liquid6112
Disclaimer/Publisher’s Note: The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.

Share and Cite

MDPI and ACS Style

Bai, B.; Liang, J.; Dai, C.; He, W.; Bai, Y.; Chang, X.; Zheng, M.; Li, H.; Zong, H. Diagenesis of the Permian Fengcheng Formation in the Mahu Sag, Junggar Basin, China. Appl. Sci. 2023, 13, 13186. https://doi.org/10.3390/app132413186

AMA Style

Bai B, Liang J, Dai C, He W, Bai Y, Chang X, Zheng M, Li H, Zong H. Diagenesis of the Permian Fengcheng Formation in the Mahu Sag, Junggar Basin, China. Applied Sciences. 2023; 13(24):13186. https://doi.org/10.3390/app132413186

Chicago/Turabian Style

Bai, Bin, Jiwei Liang, Chaocheng Dai, Wenjun He, Ying Bai, Xiaobin Chang, Meng Zheng, Hanlin Li, and Hao Zong. 2023. "Diagenesis of the Permian Fengcheng Formation in the Mahu Sag, Junggar Basin, China" Applied Sciences 13, no. 24: 13186. https://doi.org/10.3390/app132413186

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop