Mineralogical Characteristics of Early Permian Paragonite-Bearing Coal (No. 3) in the Jinyuan Mine, Tengxian Coalﬁeld, Shandong Province, Eastern China

: The Early Permian coal is of great value in the Tengxian Coalﬁeld, Shandon Province, Eastern China. This work deals with the new data focusing on mineralogical characteristics in the Early Permian Shanxi Formation No. 3 coal from the Jinyuan Mine. The Jinyuan coal is a low ash and highly volatile A bituminous coal. Minerals in the No. 3 coal mainly comprise of kaolinite, ankerite, illite, calcite, siderite, and quartz, with varying compositions of trace amounts of pyrite, jarosite, bassanite, anatase, and rutile. According to mineral assemblage in the coal plies, three Types (A to C) can be identiﬁed in the No. 3 coal. The dominant minerals in Type A are poorly-ordered kaolinite, illite, quartz, pyrite, and jarosite. Type B is mainly composed of well-ordered kaolinite, illite, siderite, ankerite, and calcite. Type C, with just one sample (JY-3-7c), which contains high proportions of calcite (54%) and ankerite (34%). Terrigenous minerals are elevated in coal plies that typically have relatively high contents of ash yield. The formation of syngenetic pyrite was generally due to seawater, while the sulphate minerals (jarosite and coquimbite) were derived from the oxidation of pyrite. Epigenetic vein-like or fracture-ﬁllings carbonate minerals (ankerite, calcite, and siderite), kaolinite, and pyrite, as well as authigenic quartz were derived from the inﬂux of hydrothermal ﬂuids during di ﬀ erent periods, from the authigenic to epigenetic. The paragonite in the coal may have been formed by the precipitated from Na-rich hydrothermal ﬂuids. No e ﬀ ects of magmatic intrusion on mineralogy were investigated in this research.


Introduction
Coal is an irreplaceable economic resource and still used as an electrical energy source, supplying the major global electricity needs around the world [1,2], especially in China, which has consumed large amounts of coal in recent years (for instance, amounting to 4.73 Gt in 2018) [3,4].
Coal is a kind of sedimentary rock and is mainly composed of organic ingredients (or macerals) and inorganic compositions [5][6][7][8], the latter of which consists of discrete crystalline particles, amorphous mineral phases, and non-mineral inorganic elements [7,8]. The study of the minerals in coal is of great significance, not only because it can be used as a critical indicator to understand the peat depositional conditions and various geologic processes during the whole period of coal formation [7,[9][10][11], but also

Geological Setting
The Tengxian coalfield is situated in southwest Shandong Province, eastern China (Figure 1), and covers an area of~1398 km 2 . The coalfield is divided into Tengbei Diggings (north area of the coalfield) and Tengnan Diggings (south area of the coalfield) based on Tengxian anticline ( Figure 1). Abundant faults have been found in Tengnan Diggings, where the east, west and south sides are surrounded by the SN-Zeshan fault, SN-Sunshidian fault, and EW-Peicheng fault, respectively ( Figure 1). The Tengnan Diggings also includes several coal mines, where the Jinyuan Mine, which is located in the southeast part of the Tengnan Diggings ( Figure 1).
The major coal-bearing units in the Tengxian coalfield are the Pennsylvanian Taiyuan Formation and the Early Permian Shanxi Formation. The Taiyuan Formation is conformably overlying of the Benxi formation (Figure 2), which was deposited in a marine-terrestrial transitional environment and is represented by an average thickness of 180 m [38]. It is mainly comprised of mudstone, siltstone, limestone, fine grained sandstone, and coal seams. There are seven coal seams in this formation, while numbers 16 and 12 are minable, and numbers 17, 14 and 8 are partly minable coal seams [38] (Figure 2).
The Early Permian Shanxi Formation is an important coal-bearing stratum in this coalfield, having a thickness varying from 80-140 m, with an average thickness of 110 m [26]. The deposited environment of the bottom section of Shanxi Formation was a marine-terrestrial transitional environment, whereas the depositional environment was transformed to a continental sedimentary environment in the subsequent deposition processes. The lithological composition of the Shanxi Formation consists of fine-medium grained sandstone, siltstone, mudstone, sandy claystone and coal seams, where the No. 3 coal is the lowermost seam and is one of the dominating mineable coal seams of the Shanxi Formation in this area [26,38] (Figure 2). In the study area, the thickness of the No. 3 coal seam varies from 1.3 to 5.1 m (2.9 m on average). In some cases, the No. 3 coal seam is split into two different coal seams, namely No. 3S and No. 3X from top to bottom, both of which are minable coal seams. The major coal-bearing units in the Tengxian coalfield are the Pennsylvanian Taiyuan Formation and the Early Permian Shanxi Formation. The Taiyuan Formation is conformably overlying of the Benxi formation ( Figure 2), which was deposited in a marine-terrestrial transitional environment and is represented by an average thickness of 180 m [38]. It is mainly comprised of mudstone, siltstone, limestone, fine grained sandstone, and coal seams. There are seven coal seams in this formation, while numbers 16 and 12 are minable, and numbers 17, 14 and 8 are partly minable coal seams [38] (Figure 2).
The Early Permian Shanxi Formation is an important coal-bearing stratum in this coalfield, having a thickness varying from 80-140 m, with an average thickness of 110 m [26]. The deposited environment of the bottom section of Shanxi Formation was a marine-terrestrial transitional environment, whereas the depositional environment was transformed to a continental sedimentary environment in the subsequent deposition processes. The lithological composition of the Shanxi Formation consists of fine-medium grained sandstone, siltstone, mudstone, sandy claystone and coal seams, where the No. 3 coal is the lowermost seam and is one of the dominating mineable coal seams of the Shanxi Formation in this area [26,38] (Figure 2). In the study area, the thickness of the No. 3 coal seam varies from 1.3 to 5.1 m (2.9 m on average). In some cases, the No. 3 coal seam is split into two different coal seams, namely No. 3S and No. 3X from top to bottom, both of which are minable coal seams.
During the later period of the Yanshan Movement (Cretaceous), frequent magmatic activities occurred in the Tengxian coalfield, especially in the Southeast of Tengnan Diggings, mainly distributed in the Zhaoyang, Jinyuan, Gaozhuang, Sanhekou, Qiwu and Tianchen coal mines ( Figure  1). From south to north, magmatic activity weakens gradually [29]. The magmatic rocks in this area can be mainly divided into three types: lamprophyre, diorite, and diabase rocks [29].

Sample Collection and Analytical Methods
Eleven stratified samples, including 10 coal plies and associated one roof samples were taken from the upper portion of the No. 3 coal seam (JY-3) at the underground working face of the Jinyuan Mine, based on the Chinese Standard Method [39]. The lowermost portion of the No. 3 coal seam and associated floor samples are unavailable due to the limitations of coal mining craft and sample During the later period of the Yanshan Movement (Cretaceous), frequent magmatic activities occurred in the Tengxian coalfield, especially in the Southeast of Tengnan Diggings, mainly distributed in the Zhaoyang, Jinyuan, Gaozhuang, Sanhekou, Qiwu and Tianchen coal mines ( Figure 1). From south to north, magmatic activity weakens gradually [29]. The magmatic rocks in this area can be mainly divided into three types: lamprophyre, diorite, and diabase rocks [29].

Sample Collection and Analytical Methods
Eleven stratified samples, including 10 coal plies and associated one roof samples were taken from the upper portion of the No. 3 coal seam (JY-3) at the underground working face of the Jinyuan Mine, based on the Chinese Standard Method [39]. The lowermost portion of the No. 3 coal seam and associated floor samples are unavailable due to the limitations of coal mining craft and sample collection capacities. Coal bench samples were collected every 20 cm along the coal seam profile from top to bottom and identified as JY-3-R, JY-3-1c, JY-3-2c, JY-3-3c, JY-3-4c, JY-3-5c, JY-3-6c, JY-3-7c, JY-3-8c, JY-3-9c, and JY-3-10c. All collected samples were immediately wrapped with hop-pocket and sealed in plastic bags.
The coal ply samples were crushed and ground to <200-mesh for the proximate and mineralogical analyses. Proximate analysis was performed using the methods of American Society of Testing Materials (ASTM) Standards [40][41][42][43][44]. Mean random vitrinite reflectance was determined using An Axio Scope.A1 microscope equipped with a Craic 508 PV spectrophotometer based on ASTM Standard D2798-20 (2020) [45].
A scanning electron microscope (SU8200, JEOL, Tokyo, Japan) in conjunction with an energy-dispersive X-ray spectrometer (SU8200, Octane Super, AMETEK, Tokyo, Japan) at the Key Laboratory of Resource Exploration Research of Hebei Province were used to determine the distribution and modes of occurrence of minerals in polished specimen. Table 1 shows the results of proximate and related analyses such as, gross calorific value, total sulfur, and mean random vitrinite reflectance of the coal ply samples from the Jinyuan Mine. The results indicate that in addition to a few low to medium ash plies from the uppermost and lower part of the section, the majority of coal plies have low ash yields (<10%). Overall, the Jinyuan coal with an average ash yield of 11.35%, which is regarded as low-ash coal based on Chinese Standard GB/T 15224.1-2010 [54]. With the exception of samples JY-3-1c and JY-3-9c, which contain high total sulfur of 1.35% and 1.04%, respectively, other coal plies are characterized by low sulfur content (Table 1). Coal samples have an average of 0.44% total sulfur, corresponding to low-sulfur coal based on the classification by Chou [55].

Coal Quality and Chemistry
Jinyuan coals are characterized by low moisture contents (1.34-1.74%, 1.54% on average) and high gross calorific values (30.76 MJ/kg on average). The volatile matter contents range from 33.32% to 47.71%, with an average of 38.95%. It should be noted that some lower-ash-yield coal plies (i.e., JY-3-2c, -4c, -7c) with highly volatile matter contents are caused by high contents of carbonate minerals, such as calcite. The mean random vitrinite reflectance is 0.76%. Therefore, the average vitrinite reflectance and values of volatile matter indicate that the Jinyuan coal is highly volatile A bituminous based on ASTM classification D388-12 (2012) [56].
Based on the mineral content and assemblage in each coal LTA sample (Table 2), three mineral assemblage types were observed in the No. 3 coals: 1.
Type A is comprised of the samples JY-3-1c and JY-3-9c, with relatively high ash yields, quartz, pyrite, and sulfate minerals (i.e., jarosite and coquimbite), while carbonate minerals (i.e., calcite, ankerite, and siderite) were not detected by XRD. The sample JY-3-1c is located in the uppermost coal section, where the JY-3-9c sample is close to the bottom of the seam.

Modes of Mineral Occurrence
The X-ray diffractograms display that the poorly ordered kaolinite is found in the Type A, while kaolinite in the Type B samples is well ordered (Figure 3). Permana et al. [57] and Wang et al. [33] have reported a similar phenomenon in some coals from the Bowen Basin and the Southwestern Shandong coalfields, respectively, and the latter is adjacent to the coals in this study. Kaolinite was observed to occur as cell-fillings ( Figure 4A), matrix intimately mixed with detrital quartz (Figure 4B), and pelletoidal fine particles (1-5 µm, Figure 4C) under the optical and SEM. Kaolinite with the former two forms mainly occured in samples from Type A. In most cases, the pelletoidal fine particles of kaolinite are distributed along bedding planes, or alternatively, assembled as irregular to ellipsoidal aggregates. This form of kaolinite is common in samples from Type B, in addition, XRD patterns show the structure of the kaolinite is well ordered in these samples, and this probably indicates that pelletoidal fine kaolinite particles are of terrigenous origin, while kaolinite is carried into (washed or blown) and preserved in the peat deposit, and subsequent diagenesis would lead to the increase in the structural order of kaolinite [58]. Trace amounts of kaolinite occur as fracture-fillings ( Figure 4D), indicating an epigenetic precipitation.   Illite present in the Jinyuan coal was mainly found to be in layers along the bedding planes ( Figure 4E,F), suggesting a detrital origin. The cell-filling paragonite ((NaAl 2 (AlSi 3 )O 10 (OH) 2 )), which was observed in few coal plies by SEM, occurs as cell-fillings, indicating an authigenic origin ( Figure 5A). In a few cases, paragonite also co-exists with kaolinite ( Figure 5B-D).
Quartz in the No. 3 coals occurs in three forms: (1) as scattered irregular grains distributed in clay matrix or organic matter, with a size commonly more than 10 µm ( Figure 4B; Figure 6A,B), indicating a detrital origin; (2) as cell-fillings ( Figure 6B) and (3) as discrete fine particles (<10 µm) embedded in collodetrinite ( Figure 6C,D). Quartz with the latter two forms suggests an authigenic origin.  Illite present in the Jinyuan coal was mainly found to be in layers along the bedding planes ( Figure 4E,F), suggesting a detrital origin. The cell-filling paragonite ((NaAl2(AlSi3)O10(OH)2)), which was observed in few coal plies by SEM, occurs as cell-fillings, indicating an authigenic origin ( Figure  5A). In a few cases, paragonite also co-exists with kaolinite ( Figure 5B-D). Quartz in the No. 3 coals occurs in three forms: (1) as scattered irregular grains distributed in clay matrix or organic matter, with a size commonly more than 10 μm ( Figure 4B; Figure 6A,B), indicating a detrital origin; (2) as cell-fillings ( Figure 6B) and (3) as discrete fine particles (<10 μm) embedded in collodetrinite ( Figure 6C,D). Quartz with the latter two forms suggests an authigenic origin.
Ankerite, calcite and siderite are the dominated carbonate minerals in the No. 3 coals. The X-ray  Pyrite was mainly detected in samples from Type A and has various modes of occurrence. It occurs as isolated or clustered framboids ( Figure 8A,B), as well as subhedral to euhedral crystals Ankerite, calcite and siderite are the dominated carbonate minerals in the No. 3 coals. The X-ray diffractogram shows that the siderite in the coal is characterized by a basal peak at 2.787 Å, which is relatively low compared to the normal siderite (2.795 Å) (Figure 3). It is thus probably identified as Mg-bearing siderite [59]. In addition, SEM-EDS study also shows that it contains a trace of Mg ( Figure 7F). Under the SEM, ankerite and calcite are mainly present as fusinite-cell-fillings ( Figure 7A,B) and vein-fillings ( Figure 7C,D), indicating an epigenetic origin [60]. Mg-bearing siderite has similar modes of occurrence to ankerite and calcite, generally occuring in fracture-fillings ( Figure 7E), suggesting that its formation is of hydrothermal origin as well.
Pyrite was mainly detected in samples from Type A and has various modes of occurrence. It occurs as isolated or clustered framboids ( Figure 8A,B), as well as subhedral to euhedral crystals ( Figure 8B,C), cell-fillings ( Figure 8D), and massive forms in the clay minerals matrix ( Figure 8E), which probably indicate syngenetic, or early diagenetic origin [8,55,61,62]. To a lesser extent, the fracture-filling pyrite, which indicates an epigenetic precipitation of hydrothermal solutions [63,64], was also observed under the SEM ( Figure 8F).
Sulphate minerals in the coals include jarosite and coquimbite, which were detected only in samples from Type A that were enriched in higher pyrite concentrations than others coal plies. Some framboidal pyrites are corroded and replaced by jarosite ( Figure 8G,H), and in some cases, the outside edge of the corroded pyrite is substituted by jarosite as well ( Figure 8I). Such modes of occurrence of the jarosite may represent an oxidation product of pyrite [8,65,66].
A small proportion of bassanite was determined by XRD analysis in several of the Jinyuan LTAs, especially those plies from Type B which have low ash yields; however, it is absent in the floor sample and samples from Type A. In some cases, the bassanite could have formed by dehydration of gypsum, while gypsum was formed by the interaction between the sulphuric acid and the Ca, which is derived from the oxidation of pyrite and released from calcite, respectively [7,[67][68][69][70]. However, bassanite in this study is not relevant to jarosite, as well as other minerals formed by pyrite oxidation, hence, the formation of bassanite is more likely due to the interaction between organically-associated sulphur and calcium during the plasma-ashing process [7,65,[71][72][73].  Pyrite was mainly detected in samples from Type A and has various modes of occurrence. It occurs as isolated or clustered framboids ( Figure 8A,B), as well as subhedral to euhedral crystals ( Figure 8B,C), cell-fillings ( Figure 8D), and massive forms in the clay minerals matrix ( Figure 8E), which probably indicate syngenetic, or early diagenetic origin [8,55,61,62]. To a lesser extent, the fracture-filling pyrite, which indicates an epigenetic precipitation of hydrothermal solutions [63,64], was also observed under the SEM ( Figure 8F). Sulphate minerals in the coals include jarosite and coquimbite, which were detected only in samples from Type A that were enriched in higher pyrite concentrations than others coal plies. Some framboidal pyrites are corroded and replaced by jarosite ( Figure 8G,H), and in some cases, the outside edge of the corroded pyrite is substituted by jarosite as well ( Figure 8I). Such modes of occurrence of the jarosite may represent an oxidation product of pyrite [8,65,66]. A small proportion of bassanite was determined by XRD analysis in several of the Jinyuan LTAs, especially those plies from Type B which have low ash yields; however, it is absent in the floor sample and samples from Type A. In some cases, the bassanite could have formed by dehydration of gypsum, while gypsum was formed by the interaction between the sulphuric acid and the Ca, which is derived from the oxidation of pyrite and released from calcite, respectively [7,[67][68][69][70]. However, bassanite in this study is not relevant to jarosite, as well as other minerals formed by pyrite oxidation, hence, the formation of bassanite is more likely due to the interaction between organically-associated sulphur and calcium during the plasma-ashing process [7,65,[71][72][73].
Trace amounts of anatase or rutile are also detected in some coal plies by using XRD. Anatase in the coals primarily occurs as scattered particles in organic matter ( Figure 9A). Albite and K-feldspar Trace amounts of anatase or rutile are also detected in some coal plies by using XRD. Anatase in the coals primarily occurs as scattered particles in organic matter ( Figure 9A). Albite and K-feldspar in the Jinyuan coal occur as discrete, irregular, angular particles distributed in the clay matrix ( Figure 9B). The similar morphology of the anatase and feldspars indicate that both have detrital origins [66,74].

Discussion: Origin of Minerals in the Jinyuan Coals
The minerals in the No. 3 coals from the Jinyuan Mine are of terrigenous, authigenic, and epigenetic origin. Three factors have been identified that affect coal mineralogical anomalies and modes of occurrence in the Jinyuan coals, including detrital input, multi-stage hydrothermal activities, and seawater influence.

Detrital Input
As mentioned above, the occurrence modes of quartz, poorly ordered kaolinite, illite, and the trace of feldspars and anatase in the Jinyuan coals, occurring as scattered particles, as well as layers along the bedding planes, indicate that they were terrigenous detrital minerals. These detrital minerals were found in the bench close to the roof or the bottom of the seam, which typically have relatively high ash yields, suggesting greater amounts of terrigenous materials influx into the accumulating peat deposit [8,75]. However, such detrital minerals are rare in the low-ash yield samples which are in the middle of the coal seam profile, where the kaolinite is abundant and mainly occurs as pelletoidal fine kaolinite (as described above). This may be due to the vegetation in or around the peat mire, which serves as a natural barrier, restraining detrital minerals, especially large quartz and feldspar particles, from penetrating into the peat swamp [6,7], however, kaolinite is fine in size, thus, it can effectively migrate into and be deposited in the peat mire [33]. Oppositely, during the formation of the uppermost coal section, the intensity of tectonic movement was increased, which affects the vegetation growth and weakens the prevention of vegetation at the same time [33], thus allowing detrital minerals to be preserved in the uppermost coal ply [33,51]. Thus, the input of the detrital minerals is one of the most prominent factors that control ash yields and mineral assemblages in the coals studied.

Multi-Stage Hydrothermal Activities
In addition to the input of the detrital minerals, multi-stage hydrothermal fluids also play a critical role in influencing the mineral anomalies in the Jinyuan coals.
Based on the modes of occurrence of minerals, kaolinite and pyrite occur as cell-fillings, suggesting an authigenic origin, these mineral phases more likely formed by the invasion of

Discussion: Origin of Minerals in the Jinyuan Coals
The minerals in the No. 3 coals from the Jinyuan Mine are of terrigenous, authigenic, and epigenetic origin. Three factors have been identified that affect coal mineralogical anomalies and modes of occurrence in the Jinyuan coals, including detrital input, multi-stage hydrothermal activities, and seawater influence.

Detrital Input
As mentioned above, the occurrence modes of quartz, poorly ordered kaolinite, illite, and the trace of feldspars and anatase in the Jinyuan coals, occurring as scattered particles, as well as layers along the bedding planes, indicate that they were terrigenous detrital minerals. These detrital minerals were found in the bench close to the roof or the bottom of the seam, which typically have relatively high ash yields, suggesting greater amounts of terrigenous materials influx into the accumulating peat deposit [8,75]. However, such detrital minerals are rare in the low-ash yield samples which are in the middle of the coal seam profile, where the kaolinite is abundant and mainly occurs as pelletoidal fine kaolinite (as described above). This may be due to the vegetation in or around the peat mire, which serves as a natural barrier, restraining detrital minerals, especially large quartz and feldspar particles, from penetrating into the peat swamp [6,7], however, kaolinite is fine in size, thus, it can effectively migrate into and be deposited in the peat mire [33]. Oppositely, during the formation of the uppermost coal section, the intensity of tectonic movement was increased, which affects the vegetation growth and weakens the prevention of vegetation at the same time [33], thus allowing detrital minerals to be preserved in the uppermost coal ply [33,51]. Thus, the input of the detrital minerals is one of the most prominent factors that control ash yields and mineral assemblages in the coals studied.

Multi-Stage Hydrothermal Activities
In addition to the input of the detrital minerals, multi-stage hydrothermal fluids also play a critical role in influencing the mineral anomalies in the Jinyuan coals.
Based on the modes of occurrence of minerals, kaolinite and pyrite occur as cell-fillings, suggesting an authigenic origin, these mineral phases more likely formed by the invasion of syngenetic hydrothermal fluids to the coal seam. The mode of occurrence of paragonite implies its authigenic origin rather than terrigenous origin. Although uncommon in coal seams, paragonite is relatively widespread in low-grade metamorphic rocks [76,77] and high rank anthracites [78][79][80], in some cases, paragonite has been found in low-rank coal areas affected by heat-induced metamorphism [65]. Wang et al. [59] noted that paragonite in the Late Permian coals from the Changxing Mine (Southwestern China) was probably a product of the dissolution and recrystallization of mixed-layer I/S during coal metamorphism. Susilawati and Ward [65] suggested that the paragonite in the coal from the Bukit Asam deposit, South Sumatra, was derived from the interaction between kaolinite and Na-bearing hydrothermal fluids. Although paragonite mostly occurs in higher rank coals, it also occurs in high-volatile bituminous Permian coal from the Sydney Basin, Australia [75]. In this study, paragonite in the No.3 coals mainly occurs as cell-fillings and co-exists with kaolinite, suggesting that paragonite in Jinyuan coals may have been derived from the precipitated by the Na-rich fluids. However, the source of Na-rich fluids warrants further investigation.
Authigenic quartz was probably syngenetically precipitated from the silicious solutions. A similar phenomenon was discovered in many Southwestern Chinese coals, such as the Xuanwei coals [81] and the Yueliangtian coals [82,83].
Epigenetic vein-like calcite, ankerite, and siderite are widely found in Jinyuan coals, especially abundant in sample JY-3-7c, which has high contents of calcite (54%) and ankerite (34%). In general, the acidic environment of normally peat-swamp is not conducive to the existence of carbonate minerals [33,73,84,85]. In most instances, the epigenetic carbonate minerals can be precipitated either from Ca (Mg, Fe)-bearing meteoric fluids or underground water during the coal-formation process. However, many scholars reported a great abundance of cleat-or fracture-fillings carbonate minerals in these coals adjacent to igneous intrusions, which are derived from hydrothermal alteration of the igneous material [86][87][88][89]. A previous study by Dai et al. [35] has noticed that high contents of calcite and dolomite in the Adaohai coals were derived from igneous fluids. However, Dai et al. [89,90] reported carbonate minerals in the Guanbanwusu and Haerwusu coals as well, located adjacent to the Adaohai coal which were not derived from igneous intrusions, because the rank of these coals are distinctly lower than the Adaohai coal. Similarly, in the present study, although frequent magmatic activity occurred in the research area during the later period of the Yanshan Movement, it appears that the carbonate minerals were not derived from igneous intrusions, because the volatile matter yield and the rank of the Jinyuan coal are close to the contemporaneous Luxi, Liangbaosi, and Tangkou coals from the adjacent coalfields [33]. Furthermore, although epigenetic vein-like carbonate minerals are abundant in sample JY-3-9c, as well as the occurrence of paragonite in this sample, the vitrinite reflectance of this sample has no obvious change compared to other coal plies, possibly indicating that the Jinyuan coal does not seem to be influenced by the apparent intrusion of magma. Therefore, the formation temperature of these epigenetic minerals such as calcite and paragonite was not too high [89].
In addition, the cell-filling calcite, fracture-filling kaolinite, and fracture-filling pyrite observed in the study coals are also due to the influx of hydrothermal fluids influx during different periods of the coal formation.

Seawater Influence
Previous studies have indicated that the peat depositional environment of the Shanxi Formation in the study area was the marine-terrestrial transitional environment at the early stage [38]. In the present study, the No. 3 coal belongs to the lower part of the Shanxi Formation, which was deposited in a lagoon environment in the Tengnan coalfield [26], in addition, studies by Chen et al. [91] have also shown that seawater affected the bottom section of the Shanxi Formation.
High concentrations of sulfur and the presence of syngenetic pyrite in coals are used to indicate a depositional environment under the influence of seawater by many scholars [11,33,55]. Chou [55] noticed that the sulfur in low sulfur coal (<1%, total sulfur) is derived mainly from parent plant material. In the present study, the sulfur concentration varies from 0.02% to 1.35%, the average sulfur content is lower than 1%, however, it should be mentioned that a relatively high sulfur content has been found in some coal plies, especially in the uppermost coal section (JY-3-1c, 1.35%). In addition, the morphology characteristics of pyrite are framboids, euhedral crystals, and massive form that observed in these high sulfur content samples, indicating a syngenetic origin. Hence, some high-sulfur coal samples in the No. 3 coal are more likely to be affected by intermittent seawater influence during peat forming. Previous studies on contemporaneous coals from the adjacent three coalfields (Southwestern Shandong), with the same content and distribution characteristics of sulfur, also support that the seawater intrusion occurred on a large scale during this period [33].

Conclusions
The Early Permian coal from the Jinyuan Mine in Shandong Province, Eastern China is a highly volatile A bituminous coal, with low-ash and low-sulfur contents. Minerals identified in the Jinyuan coals mainly represented by kaolinite, ankerite, illite, calcite, siderite, quartz, and trace amounts of pyrite, jarosite, bassanite, anatase, and rutile. The kaolinite, quartz, and illite were derived from terrigenous materials during peat accumulation. The formation of syngenetic pyrite is generally induced by seawater, while the sulphate minerals (jarosite and coquimbite) were produced by pyrite oxidation. The modes of occurrence of carbonate minerals indicate they were formed by the precipitation of the Ca, Mg, or Fe-bearing fluids. The paragonite in the coal is probably precipitated from Na-rich fluids, while the origin of this Na-rich hydrothermal warrants further investigation. Effects of magmatic intrusion on mineralogy were not investigated in this paper, in addition, the formation temperatures associated with the carbonate minerals were not high enough to raise the vitrinite reflectance.