1 Introduction

After coal mining, a large number of gobs are formed at different mining levels. With the end of the disturbance of overburden strata, the gob tends to be stable and a large void space is formed, which provides space for mine water storage due to the impermeability of the floor. The underground reservoir is a water conservancy project with the emphasis on storage capacity, which is formed by the gap between the rock and soil as the water storage space. It is a systematic project of artificial recharge of groundwater, underground storage of water resources, and human activities of exploitation (Du et al. 2008). Since coal mines are usually located in a region where water resources are scarce or severely deficient, the use of underground reservoir is of great significance for water resources protection and ecological environment protection (Chen 2018). Compared with surface reservoirs, groundwater reservoirs have the advantages of high safety, low investment, no land occupation, and no siltation (Lan et al. 2010).

The problem of water quality in groundwater reservoirs is mainly the impact of recharged water on groundwater environment, the impact of groundwater environment on recharged water sources, and the changes in water quality of recharged water in the process of groundwater storage (Wang et al. 2018). The change of water quality of recharge water can directly affect the efficiency and operating cost of groundwater purification, and service life of groundwater reservoir (Du et al. 2018). The research of Liu (2016) shows that the changed ion content of groundwater and weakened rocks, can be powerful evidence for the process of water–rock interaction. Therefore, not only the water source prediction, site storage capacity, dam construction, and safety of coal mine groundwater reservoir need to study, but also the control of water quality of coal mine groundwater reservoir.

Due to changes in groundwater circulation patterns and water–rock interactions, the hydrogeochemical environment in the mining area has undergone tremendous changes (Feng et al. 2019a, b). Gu (2015) found through simulation experiments that the reduction of suspended solids, calcium ions, and COD concentration in mine water is related to the solid–liquid coupling effect of the fallen rock and liquid. Hu et al. (2016) found that mine water immersion has the greatest impact on the microstructure of mudstone. They also explained that the reason may be that the chemical environment is different. On the one hand, the ion environment in the mine water is complex and then content of ion is high, which causes a large amount of ion exchange between the micro-crack and the solution, which will destroy some of its chemical bonds and destroy its microstructure. On the other hand, the pH and Eh of the mine water itself promoted the destruction of micro-fractures in the mudstone. Li et al. (2008) explored the water–rock interaction mechanism of mine water in the process of saturated coal rock infiltration. During the infiltration process of the mine water, the total hardness, SO42−, and Cl− are first adsorbed by the rock at the beginning. Soon after the adsorption equilibrium is reached, dissolution, resolution, and ion exchange occur, and the dissolution rate is large at the beginning and then gradually decreases until it reaches zero. Lin et al. (2012) analyzed the changing trend of the main solute components of groundwater and the related water–rock reaction during the artificial recharge process through indoor simulation experiments. The results show that the main ionic components of groundwater are mainly affected by mixing, cation exchange adsorption, and dissolution of aquifer mineral facies (calcite, dolomite, and potassium feldspar). As a natural water storage container, groundwater reservoir can solve the problem of mine water supply and drainage, sewage treatment, flood prevention, environmental protection, and energy conservation and emission reduction if reasonably utilized. To ensure mine water resources safe and efficiently utilized, water–rock interaction is one of the most important factors. Studying the composition of the fallen roof minerals accumulated in the groundwater reservoir and its changes under the action of water–rock is the key point to understand the purification mechanism of the underground mine reservoir and control the water quality of the underground reservoir.

Basic geology and mineral resources, groundwater environment evolution and global changes, migration of trace elements in aqueous systems, transformation and enrichment, effects of water chemistry and rock mechanics, and groundwater pollution control and restoration are current research focuses in the field of rock interactions, (Shen et al. 2012; Wang et al. 2015). Goren et al. (2011) found out through indoor simulation experiments that the main controlling factors of artificial recharged wastewater and calcareous sandstone sedimentary water are cation exchange and CaCO3 dissolution. Zhang et al. (2011) conducted experiments to simulate interaction between different proportions of wastewater and carbonate rocks and the analysis shows that heavy metal salt solution has a dissolution effect on carbonate rock, and can produce secondary minerals. Deng et al. (2019) designed an indoor immersion-air-drying cycle test to monitor water pressure rise and fall and used SEM electron microscopy to analyze sandstone microscopic structure. The results show that the sandstone surface of the first six immersion-air-drying tests is particularly effective, and the sandstone surface develops from dense to irregular honeycomb structure. Gu (2018) studied the fracturing fluid-shale interaction mechanism in shale gas reservoirs during hydraulic fracturing through laboratory experiments and hydrogeochemical software simulation. Wang (2017); through the combination of theoretical analysis, laboratory test, and numerical analysis, studied the water degradation effect on rock and the mechanism of rock deformation and failure, and established a constitutive model of water-bearing rock. Zhu (2017) independently developed the rock gaseous water adsorption test system, studied the gaseous water adsorption characteristics of the sample, and combined the SEM scanning experiment and X-ray diffraction experiment to analyze the influence of clay minerals and voids and fissures on the adsorption of gaseous water.

These research results show that in the role of water and rock, the change of lithofacies is crucial to the composition of water bodies. The groundwater–rock interaction simulation is mostly completed by indoor simulation experiments. The characterization of rocks is mostly by electron microscopy and X-ray diffraction. At present, most scholars’ research focuses on the study of underground aquifers in conventional groundwater or artificial recharge areas. Research on the water–rock interaction in coal mine groundwater reservoirs is rare. The law of the change of the mineral composition of the fallen rock and the water quality of coal mine groundwater reservoir has not been systematically analyzed.

This paper focuses on studying the fallen rock in the underground reservoir of Daliuta Coal Mine. Based on previous studies on the geology and hydrogeology of the study area, this research is to determine the mineral composition of the fallen rock sample and the characteristics of the water quality of the inflow and outflow of the coal mine groundwater reservoir. Simulation experiments are designed to simulate the long-term contact of rock samples of different lithologies with mine water under coal mine conditions. The change of rock mineral composition and its structure are analyzed, and then its impact on the water quality in the groundwater reservoir. This research lays a solid foundation for the research on key technologies of mine water recycling in the subsequent underground reservoirs, the regulation of water resources in mining areas, and the protection of water supply and environmental impact assessment of mine groundwater.

2 Materials and methods

2.1 Overview of the study area

The Daliuta Coal Mine in Shendong Mining Area is located in the northwest of Shenmu County, Yulin City, Shaanxi Province. The geographical coordinates are: N39° 13′ 53″–39°21′ 32″ and E110° 12′ 23″–110° 22′ 54″. The area of Daliuta Coal Mine is approximately 126.80 km2.

The depth of the groundwater reservoir of Daliuta Coal Mine is about 130 m from the surface. Three underground reservoirs of No. 1, 2, and 3 were built using the horizontal 2−2 coal seam gob, and two recycling diverticulum were built in the second level 5−2 coal gob, and No. 4 underground reservoir is being constructed. At present, only the water of the aquifer is replenished, and the sewage is not recharged (Chen et al. 2016).

Through the simulation experiments and on-site measurement, the water storage coefficient of the underground reservoir of Daliuta Coal Mine is 0.15–0.20. The current water storage capacity of No. 1, 2 and No. 3 Reservoir is about 3.36 × 106 m3, 1.93 × 106 m3 and 1.82 × 106 m3, respectively (Chen et al. 2016).

2.2 Sample collection and preservation

Since the 2−2 coal seam has been mined and three underground reservoirs have been built, it is impossible to collect rock samples that have fallen into the underground reservoirs No. 1, No. 2 and No. 3. To obtain a similar sample, the mineral sample of the 5−2 coal seam falling roof was collected, and the experimental mineral composition was subsequently constructed according to the 2−2 coal seam borehole data. The locations of collection points of the water inflow and outflow of the coal mine underground reservoir is shown in Fig. 1. According to the actual situation of the site, select the sampling points allowed by the conditions. One water inlet and two water outlets are selected in No. 1 underground reservoir of seam 2−2, as 22,406, 400, 406, respectively. And No. 2 underground reservoir of seam 2−2 is the same, as 201, 608, 615, respectively. Fissure water and water samples of inlet 5−2 in No.2 underground reservoir are selected in 5−2 coal seam. Sampling scheme design and technology are strictly in accordance with the industry standard “Water Quality Sampling Technical Guidance” (HJ 494–2009) and “Water Quality Sampling Scheme Design Technical Regulations” (HJ 495–2009). The pH was measured on-site. Na+, Mg2+, K+, Ca2+, suspended solids (SS), Total dissolved solids (TDS), Chemical Oxygen Demand (COD), Cl−, SO42−, and F− were determined in the laboratory after pretreating the water sample and preserved in a dark place at 1–5 °C.

Fig. 1
figure 1

Water sample collection location

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One water inlet and two water outlets are selected in No. 1 underground reservoir, as 22, 406, 400, 406, respectively. And No. 2 underground reservoir is the same, as 201, 608, 615, respectively.

2.3 Simulation experiment design and parameter selection

According to the drilling log of the mine area where the underground coal reservoir is located and the rock samples taken at the site, the fallen rock in the underground reservoir is mainly sandstone and mudstone. Therefore, fine sandstone and mudstone with parallel bedding are selected as the main research objects. According to the analysis of Zhang et al. (2013) of the 12,201 gob, Laoliupan and 22,613 gob in Daliuta Coal Mine, the average filter height is 3.50 m, the distance between the average pumping hole and the water injection hole is 1100 m, the average slump rock fracture maximum block size (diameter) is 600 mm, and the water storage coefficient (Chen 2016) is between 0.15 and 0.25.

The water–rock sample was prepared in a 1000 mL beaker which was placed in an isothermal chamber. The two rock samples, fine sandstone and mudstone with parallel bedding, were crushed to 2–12 mm with a jaw crusher and then mixed with the mine water sample with the water–rock mass ratio of about 1:2. To ensure that the experimental environment is close to the operating conditions of the coal mine groundwater reservoir, the temperature was controlled as 25 °C (micro-reducing condition). The experiment setup after connecting agitator is shown in Fig. 2. One group was set as control experiment and the other group was set of blank control experiments. After soaking in the mine water for 47 days (Tang et al. 2018), the rock samples after the immersion were taken out and ground to about 300 mesh for testing.

Fig. 2
figure 2

Simulation experiment setup for water–rock interaction in groundwater reservoir

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2.4 Sample testing and analysis

The rock sample collected in the Daliuta Coal Mine and the sample after the simulation test were ground to about 300 mesh. The D/max-2500v/pc type X-ray diffractometer (XRD) (Cu target, Kα radiation, step size of 0.02°, power of 40 kV, 150 mA, continuous scanning) produced by Rigaku Corporation of Japan was used for mineral composition analysis. The following test conditions were used: 2θ angle range is 5°–70° and scanning speed is 4°/min. Using ultrasonic high-resolution thermal field emission scanning electron microscope (SEM) of Japan JSM-7610F (magnification of 0.25 to 1 million times), the rock samples which are crushed and screened to less than 75 μm are magnified to 3–30 μm. The ASAP 2020 M Rapid Specific Surface/Pore Analyzer (BET) was used to determine the specific surface area, total pore volume, and average pore size of the two types of rock samples, parallel layered mudstone and fine sandstone in Daliuta Coal Mine. The determination of specific surface area is based on the BET test method, and the pore volume and pore size distribution utilize the BJH theory. The instrument has a specific surface area measurement range of 0.005 m2/g to infinity, a pore size distribution measurement range of 0.35 to 500 nm (using H–K or DA analysis), and a minimum pore volume analysis of 0.0001 cc/g (using H–K or DA analysis).

According to the “groundwater quality inspection method” (DZ/T0064–1993) (Ministry of Geology and Mineral Resources of the People’s Republic of China 1994), the pH of the water sample was measured by portable water quality multi-function parameter tester on-site immediately after the sample was collected, and the remaining water quality indicators were tested in laboratory. Part of the water sample was sealed and stored for subsequent experimental analysis after filtered with a 0.45 μm filter. COD was determined by potassium dichromate titration. The water sample was oxidized by potassium dichromate standard solution. After heating and refluxing, the standard solution of ammonium ferrous sulfate was used to drop back. SS and TDS were determined by gravimetric method. Fully mixed 100 mL of water sample for suction filtration, washed them with 10 mL of distilled water for three times continuously, and weighed the filtrate and membrane respectively to obtain the TDS and SS. CO32− and HCO −3 were determined by titration (Liu 1981). Added drop phenolphthalein indicator and titrated with 0.05 mol/L HCl standard solution until the red color disappeared. Then added methyl orange indicator and titrated with HCl until the solution changes from yellow to orange. Anions such as Cl−, SO42−, NO −3 , and F− are determined by ion chromatography (IC) (Ministry of Environmental Protection of the People’s Republic of China 2016). The following chromatographic conditions were used: concentration of sodium carbonate of 0.0018 mol/L, concentration of sodium bicarbonate of 0.0017 mol/L, injection volume of 25 μL, eluent flow rate of 1.0–2.0 mL/min, and regenerant flow rate determined according to eluent flow rate. Conventional cations such as K+, Na+, Ca2+, Mg2+ were determined by inductively coupled plasma mass spectrometry (ICP-MS) (Ministry of Geology and Mineral Resources of the People’s Republic of China 2015).

Determine the composition of minerals in a sample was conducted using Jade 6.0 (MDI, Livermore, CA, USA) in conjunction with the material standard powder diffraction data (PDF 2004) provided by the Powder Diffraction Consortium International Data Center (JCPDS-ICDD).

3 Results and discussion

3.1 Analysis of rock formation and water quality in coal mine groundwater reservoir

It can be seen from Table 1 that the influent and effluent of coal mine underground reservoir is neutral or alkaline, the main cations in the water sample were Na+, Ca2+ and the average content was 168.27 mg/L and 158.61 mg/L; and the main anions were Cl− and SO42−, the average content was 293.16 mg/L and 344.93 mg/L, respectively. Compared with the influent, the suspended solids in the effluent are obviously reduced, the total hardness is reduced, Na+ and Cl− increase, and COD, Ca2+, Mg2+, HCO −3 and SO42− decrease. The change of K+ and Mg2+ is not obvious because of the lower content. According to Shukarev’s nomenclature, the type of water chemistry changes from influent type 36-A (SO42−·Cl−-Ca2+) to effluent type 42-A (SO42−·Cl–Na+) (Han et al. 2016; Zhang et al. 2019. Referring to the “Standard for Groundwater Quality” (GB/T14848–2017), although the water quality of influent and effluent in groundwater reservoir generally conforms to the quality standard for class V groundwater, compared with the influent quality, the effluent quality has been significantly improved.

Table 1 Chemical analysis of coal mine groundwater reservoir (mg/L)
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Ma and Wang (2017) and Xu et al. (2019) believed that water–rock interaction is the dominant feature of water chemistry in the study area, and the water body ions are significantly affected by water–rock interaction. According to the change of hydrochemical characteristics of water, it indicates that there is water–rock interaction in coal mine underground reservoir, and the hydrochemical characteristics of effluent water are closely related to the fallen rocks in coal mine groundwater reservoir. Therefore, further study of the mineral composition in the groundwater reservoir is a necessary step to reveal the water–rock interaction.

The minerals in the underground reservoir of coal mine mainly come from the collapse of the roof and its overlying strata. Thus, the composition and distribution characteristics of the overlying strata are the basis for studying the mineral composition in the reservoir. The average buried depth of the groundwater reservoirs in No. 1 and No. 2 of Daliuta Coal Mine is 93.57–104.09 m, with an average of 98.83 m. The distance between the groundwater reservoirs and Quaternary strata is 62.56–66.80 m, with an average of 64.68 m (Chen et al. 2016; Gu 2012; Li et al. 2017) (Fig. 3). The overlying lithology of No. 1 underground reservoir is mainly sand-mud interbedded layer, with multiple coal-bearing lines. The thickness of mudstone accounts for about 27% of the total thickness of the overlying strata of No. 1 groundwater reservoir, and the thickness of sandstone accounts for about 72%. The thickness of the 2−2 coal seam of No. 1 groundwater reservoir is 4.21 m, and the rock layers adjacent to the upper part are interbedded with siltstone and medium sandstone, respectively, with a total thickness of 22.40 m (Fig. 3a). The distribution of No. 2 groundwater reservoir is similar to that of No. 1, with mudstone thickness accounting for about 30% and sandstone thickness accounting for about 70%. The thickness of the 2−2 coal seam of No. 2 groundwater reservoir is 4.71 m, and the rock layers adjacent to the upper part are mudstone, siltstone and fine sandstone, respectively, with total thicknesses of 2.46 m, 1.14 m and 5.39 m, respectively, totaling 8.99 m (Fig. 3b). In summary, the overlying lithology of coal mine groundwater reservoirs in the study area is mainly sandstone, including siltstone, fine sandstone and medium sandstone, accounting for about 70%; followed by mudstone, including mudstone and carbonaceous mudstone, accounting for about 30%.

Fig. 3
figure 3

Drilling log of No. 1 and No. 2 Underground Reservoir

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Fu et al. (2018) studied in the Huai’nan Xinji mining area and found that Cl− and Na+ are the main sources of TDS in sandstone water, Na+, Ca2+, Mg2+, and Cl− are related, Na+ and Ca2+, Mg2+ have alternating adsorption, and Na+ and Cl− may be from the dissolution of rock salt. Yan et al. (2014) used the tap water to soak the mudstone of the Xinzhuang Coal Mine and found that the largest relative change is S and CaO. Studies of Zhang et al. (2018) have shown that the lithology of the 10 coal seams floor of Haishu Mine is light gray fine sandstone and dark gray-grey black mudstone and siltstone interbed, and the roof is light gray medium-fine quartz sandstone. The ion content of sandstone water in the roof and floor is obviously different. The hydrochemistry type of coal measures sandstone in the floor is mainly Ca2+·Mg2+-SO42−, and the hydrochemistry type coal measures sandstone in the roof is mainly HCO −3 ·Cl−. The water quality has changed obviously, and the change is related to the mineral properties of rocks, that is, the water quality is controlled by the fallen rocks in the underground reservoir. Therefore, the concentration of major ions in the waters of the study area has changed, and the water quality has been significantly improved. It is speculated that the water–rock action of the reservoir water and the fallen rock changes the ion content of the water.

3.2 Characteristics Analysis of Mineral Structure of Coal Mine Groundwater Reservoir

In order to further analyze the main sites of water–rock reaction and the influence of mineral surface changes on water–rock interaction, the morphology was characterized by scanning electron microscopy and the specific surface area and pores of rock samples were determined by nitrogen adsorption. The results are shown in Figs. 4, 5 and Table 2.

Fig. 4
figure 4

SEM morphology of rock samples in gobs

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Fig. 5
figure 5

SEM morphology of rock samples after simulation experiment

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Table 2 Surface structure and pore distribution of mudstone and sandstone in underground reservoir
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Before the action of water–rock, the sandstone and mudstone surface showed a flocculent porous structure with layered silicate structure and flaky kaolinite (Fig. 4). After the mine water passes through the reservoir sedimentation and water–rock action, the mineral surface structure became dense and the porous structure disappears (Fig. 5). Due to the development of pores and micro-cracks in clay minerals, the surface area increases, which enhances its adsorption capacity. Moreover, the granularity of the fallen sandstone in the underground reservoir of the coal mine is good, and the particles are closely arranged, which has a good filtration and adsorption effect on the mine water. Engineering practice (Gu 2015; Chen et al. 2016; Cao et al. 2014) and Table 1 show that with the increase of water–rock action time, the minerals on the rock surface are coupled with the mine water, the SS of the groundwater reservoir is greatly reduced, the COD is slightly reduced, and the water quality is changed. The content of albite and some clay minerals is reduced, so that the adsorption capacity of the rock surface is slowly weakened. The above analysis indicates that the mineral surface structure is the main site of adsorption, transition and water–rock action, and it is also the key to water purification. The mineral surface structure and pore distribution change after water–rock interaction, which affects the subsequent purification effect of mine water.

The specific surface area of the rock sample was 7.18–9.93 m2/g with a mean of 8.56 m2/g. The pore volume was 0.03–0.04 cc/g, with the average value of 0.035 cc/g. The pore size distribution was 15.62–17.55 nm and the average pore size was 16.59 nm, which was a mesoporous (Table 2). Compared with mudstone, the specific surface area of sandstone is obviously higher, the total pore volume is slightly higher, but the average pore diameter is opposite. Comparing the findings with those of other researchers, there is a commonality. Zhu (1996) has shown that the thickness of water-absorbing film formed by water on the pore surface of rock is different due to the difference of mineral composition, generally greater than 0.10 μm. Guo et al. (2016) found that the influence of rock structure is mainly manifested in the development degree of surface micro-cracks, the more the surface micro-cracks develop, the stronger the adsorption. From the results, the fallen rock in the underground mine of the coal mine in the study area can only form a water-absorbing membrane on the surface, and there is no easy flow of water inside the rock. The adsorption, filtration and sedimentation of suspended solids and other substances in the mine water are mainly located at the joints and voids formed after the stress changes in the upper strata.

Engineering practice (Gu 2012) shows that, the Daliuta coal mine’s mining ratio and crack mining ratio are about 3–4:1 and 25–30:1 respectively. With the exploitation of coal, the overburden layer of the 2−2 coal seam is severely deformed, forming a large gap. The minerals in the underground reservoir of coal mine are mainly siltstones, mudstones, and their interbedded rock groups and sandstone formations. The lithology above them is also dominated by glutenite. The slump formed by siltstone and mudstone has a fine particle size and is easily muddy under the action of water, so that the particle gap becomes smaller. The latter is dominated by medium-grained sandstone and fine-grained sandstone, and part is coarse-grained sandstone, and the formed slump has a large grain size. Therefore, the particle gradation of the litter in the gob of the study area is good. The particles are arranged closely, the sandstone in the crack zone and caving zone plays a natural filtering effect. The gap between the fallen rocks and the water absorbing film formed on the surface plays a key role in water purification.

In summary, the surface structure of the mineral phase and the pores formed on the surface are the main sites for adsorption, filtration and water–rock interaction in the process of water purification, and are also the key to water purification. However, with the increase of interaction time between the fallen rock and the mine water, the surface structure of mineral phase and the pores formed on its surface will also change, so that its purification effect on mine water will slowly be weaken. Therefore, it is necessary to timely clean up the sludge deposited in the bottom of the reservoir to ensure the service life of the underground reservoir and its purification capacity.

3.3 Analysis on the change mechanism of mineral composition in coal mine groundwater reservoir

To further analyze the mineral composition, mudstone and sandstone samples were characterized and the results were shown in Fig. 6 and Table 3. The main minerals of the rock sample included quartz (SiO2), kaolinite (Al2O3·2SiO2·2H2O), albite (NaAlSi3O8), orthoclase (K(AlSi3O8)), illite ((K,H3O)(Al,Mg,Fe)2(SiAl)4O10 [(OH)H2O]) and chlorite (Fig. 6). There are differences in the composition of the three rock samples of sandstone, mudstone, and parallel layer mudstone, but they are basically close. Among them, quartz is the most common mineral in coal-bearing rock formations, with the highest content. Kaolinite, illite, and chlorite are the main components of clay minerals. The others are also common minerals that coexist with coal (Wang et al. 2009; Liu et al. 2017; Zhang et al. 2017). In the underground reservoir of the coal mine, the average content of quartz in the sandstone was 31.40%; feldspar was 44.30%,which were mainly albite (NaAlSi3O8) and orthoclase (K(AlSi3O8)); clay mineral was 19.5%; and with a small amount of ordinary pyroxene. The mudstone was mainly composed of clay mineral and quartz, in which the clay mineral content was about 31.3%, quartz was 41.0%, albite was 20.3%, orthoclase was less, about 7.4% (Table 3). It can be seen from Fig. 7 that compared with mudstone, sandstone had less quartz, more orthoclase and less chlorite. According to the above analysis, the proportion of sandstone and mudstone is about 7:3. It can be calculated that the content of quartz is about 34.28%, albite is 21.84%, orthoclase is 17.48%, kaolinite is 8.00%. After the mine water immersion simulation experiment, it is 36.14%, 17.87%, 11.62% and 16.75%, respectively; after the deionized water immersion simulation experiment, it is 35.47%, 19.01%, 14.49% and 12.46%, respectively. It can be seen that when the mine water flows through the underground reservoir, the mineral composition of the fallen rock will change, which in turn will affect the water quality of the underground reservoir.

Fig. 6
figure 6

Analysis of mineral composition of rock samples

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Table 3 Mineral composition and content of fine sandstone (%)
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Fig. 7
figure 7

Mineral composition of rock samples

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In the process of water and rock, the content of unstable minerals (calcite, dolomite, hornblende, etc.) and sub-stable minerals (potassium feldspar, muscovite, illite, etc.) will gradually decrease, and the proportion of stable minerals (quartz, kaolinite, Oxide or hydroxide, etc.) will increase (Vincent et al. 2018; Zhang et al. 2007; Sun et al. 2012). Deionized water immersion is to study the change of minerals in rock samples in non-ionized water. Mine water immersion experiment is to study the changes of minerals in the actual underground reservoirs, and to compare and analyze the influence of mine water on rock minerals (Yan et al. 2014). Compared with the original sandstone, the content of albite and orthoclase decreased after the immersion in mine water and deionized water, kaolinite increased, illite increased slightly, and pyrite and siderite decreased slightly after soaking in mine water and deionized water (Table 3, Fig. 8). Compared with the original mudstone, the content of albite and orthoclase decreased, and kaolinite, illite and chlorite increased slightly after soaking in mine water and deionized water (Table 3, Fig. 9). The increase and decrease of the mineral content in sandstone soaked in mine water is higher than that in deionized water, while the mudstone is opposite. The change of mineral content in sandstone is more obvious than that in mudstone. It indicates that water–rock interaction occurs, such as dissolution of albite and orthoclase, kaolinite precipitation and oxidation–reduction of pyrite and siderite, and the process of water–rock interaction is related to the chemical composition of water and the composition and content of rock minerals.

Fig. 8
figure 8

The changes of mineral content in sandstone after the experiment

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Fig. 9
figure 9

The changes of mineral content in mudstone after the experiment

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The reaction patterns of different minerals and mine water are different. Feng et al. (2019a, b) studied the interaction between Gangyi spring water and stratigraphic rocks. Under the action of water and rock, calcium montmorillonite, chlorite, and illite are formed. Illite is transformed from calcium montmorillonite, and chlorite is composed of mica mineral alterations or potassium feldspar conversion. Wang et al. (2019) studied the tight sandstone kaolinite in the fourth member of the Xujiahe Formation in the western Sichuan depression. It was found that the atmospheric fresh water and coal-series acidic water caused the feldspar to dissolve in the early diagenetic stage and formed the authigenic kaolinite. With the increase of burial depth and the increase of ground temperature, some kaolinite reacted with potassium feldspar to form illite. Gu (2018) studied the fracturing fluid-shale interaction and found that the high content of Mg2+ (Ca2+) in the solution easily caused (de)dolomite formation during the reaction, and the H+ produced by the oxidation of pyrite can promote the dissolution of carbonate minerals. NaCl solution can promote the dissolution of pyrite and inhibit the dissolution of feldspar, while CaCl2 and MgCl2 can promote the dissolution of illite and increase the precipitation of montmorillonite and chlorite.

Wandrey et al. (2011) used long-term carbon dioxide exposure experiments with fresh core materials from reservoirs. The results show that the mineral phases (non-plagioclase, potassium feldspar, anhydrite, etc.) are dissolved, which are expressed as the concentration increases of Ca2+, Mg2+, K+ and SO42−. The underground reservoir of the coal mine belongs to a humid semi-enclosed environment. Due to the occurrence of hydrolysis, OH− ions combine with metal cations and enter the underground reservoir of the coal mine to increase the pH value of the water body. H+ is mainly combined with an aluminosilicate complex anion to form a poorly soluble clay mineral which is deposited on the bottom of the water. According to the previous research results, the following change process can be inferred based on the analysis of water quality in and out of the reservoir and the change of mineral characteristics with the action of water–rock. The orthoclase and albite can be dissolved at 25 °C and atmospheric pressure, and the chlorite precipitates (shown in Eq. (1)–(4)). The dissolution of silicate minerals (albite, orthoclase and illite, etc.) is the main source of Na+, and the cation exchange reaction exchanges Ca2+ and Mg2+ in water. The main reason is that when clay (or colloid) adsorbs with Na+ and meet free (including freely ionizable) Ca2+, the clay mineral releases Na+ and adsorbs Ca2+, which causes relative excess of Na+ to Cl− and Ca2++Mg2+ relative deficiency to HCO −3 + SO42− (shown in Eq. (5)–(6)). And with the extension of the reaction time, the value of sodium adsorption ratio (SAR) gradually increases, and the cation alternate adsorption between the aqueous phase and the rock phase gradually weakens. The dissolution of feldspar will produce authigenic kaolinite, and the presence of K+ will cause the reaction of authigenic kaolinite to illite again (shown in Eq. (7)–(9)). Mg2+ and Ca2+ in the aqueous phase form montmorillonite, and when K+ is sufficient, it is converted into illite (shown in Eq. (10)–(11)). Sulfur-containing oxides (mainly pyrite) and siderite undergo oxidation reaction, and calcium-containing magnesium oxides are neutralized (shown in Eq. (12)–(17)). These reaction formulas are presumed to be as following:

$$2{\text{NaAlSi}}_{3} {\text{O}}_{8} + 2{\text{H}}_{2} {\text{CO}}_{3} + 9{\text{H}}_{2} {\text{O}} \to {\text{Al}}_{4} \left( {{\text{Si}}_{4} {\text{O}}_{10} } \right)\left( {\text{OH}} \right)_{8} + 2{\text{Na}}^{ + } + 2{\text{HCO}}_{3}^{ - } + 4{\text{H}}_{4} {\text{SiO}}_{4}$$
(1)
$$4{\text{KAlSi}}_{3} {\text{O}}_{8} + 6{\text{H}}_{2} {\text{O}} \to {\text{Al}}\left[ {{\text{Si}}_{4} {\text{O}}_{10} } \right]\left[ {\text{OH}} \right]_{8} + 8{\text{SiO}}_{2} + 4{\text{KOH}}$$
(2)
$${\text{CO}}_{2} + {\text{CaCO}}_{3} + {\text{H}}_{2} {\text{O}} \to {\text{Ca}}^{2 + } + 2{\text{HCO}}_{3}^{-}$$
(3)
$${\text{KAlSi}}_{3} {\text{O}}_{8} + {\text{Fe}}^{3 + } + {\text{Mg}}^{2 + } + {\text{H}}_{2} {\text{O}} \to {\text{Chlorite}} + {\text{SiO}}_{2} + {\text{H}}^{ + } + {\text{K}}^{ + }$$
(4)
$${\text{Ca}}^{2 + } + {\text{HCO}}_{3}^{ - } + {\text{Na}}^{ + } \left( {\text{rock}} \right) \to {\text{Na}}^{ + } + {\text{HCO}}_{3}^{ - } + {\text{Ca}}^{2 + } \left( {\text{rock}} \right)$$
(5)
$${\text{Mg}}^{2 + } + {\text{HCO}}_{3}^{ - } + {\text{Na}}^{ + } \left( {\text{rock}} \right) \to {\text{Na}}^{ + } + {\text{HCO}}_{3}^{ - } + {\text{Mg}}^{2 + } \left( {\text{rock}} \right)$$
(6)
$${\text{KAlSi}}_{3} {\text{O}}_{8} + {\text{H}}^{ + } + {\text{H}}_{2} {\text{O}} \to {\text{Al}}_{2} {\text{Si}}_{2} {\text{O}}_{5} \left( {\text{OH}} \right)_{4} + {\text{SiO}}_{2} + {\text{K}}^{ + }$$
(7)
$${\text{NaAlSi}}_{3} {\text{O}}_{8} + {\text{H}}^{ + } + {\text{H}}_{2} {\text{O}} \to {\text{Al}}_{2} {\text{Si}}_{2} {\text{O}}_{5} + {\text{SiO}}_{2} + {\text{Na}}^{ + }$$
(8)
$${\text{KAlSi}}_{3} {\text{O}}_{8} + {\text{Al}}_{2} {\text{Si}}_{2} {\text{O}}_{5} \left( {\text{OH}} \right)_{4} \to 2{\text{SiO}}_{2} + {\text{KAl}}_{3} {\text{SiO}}_{10} \left( {\text{OH}} \right)_{2} + {\text{H}}_{2} {\text{O}}$$
(9)
$${\text{Feldspar}} + {\text{H}}_{2} {\text{O}} + {\text{Ca}}^{2 + } + {\text{H}}^{ + } + {\text{Mg}}^{2 + } \to \left( {{\text{K}}^{ + } + {\text{Na}}^{ + } } \right) + {\text{SiO}}_{2} + {\text{Montmorillonite}}$$
(10)
$${\text{Montmorillonite}} + {\text{K}}^{ + } + {\text{Al}}^{3 + } \to {\text{Illite}} + {\text{Na}}^{ + } + {\text{Ca}}^{2 + } + {\text{Fe}}^{3 + } + {\text{Mg}}^{2 + } + {\text{Si}}^{4 + }$$
(11)
$${\text{FeS}}_{2} + {\text{O}}_{2} + {\text{H}}_{2} {\text{O}} \to {\text{Fe}}^{2 + } + {\text{SO}}_{4}^{ - } + {\text{H}}^{ + }$$
(12)
$${\text{FeS}}_{2} + {\text{O}}_{2} + {\text{H}}_{2} {\text{O}} \to {\text{Fe}}^{3 + } + {\text{SO}}_{4}^{ - } + {\text{H}}^{ + }$$
(13)
$${\text{FeS}}_{2} + {\text{O}}_{2} + {\text{H}}_{2} {\text{O}} \to {\text{Fe}}\left( {\text{OH}} \right)_{3} \left( {\text{s}} \right) + {\text{SO}}_{4}^{ - } + {\text{H}}^{ + }$$
(14)
$${\text{FeCO}}_{3} + {\text{O}}_{2} + {\text{H}}_{2} {\text{O}} \to {\text{Fe}}\left( {\text{OH}} \right)_{3} \left( {\text{s}} \right) + {\text{H}}^{ + } + {\text{HCO}}_{3}^{ - }$$
(15)
$${\text{CaCO}}_{3} + {\text{H}}^{ + } \to {\text{Ca}}^{2 + } + {\text{CO}}_{2} \left( {\text{g}} \right) + {\text{H}}_{2} {\text{O}}$$
(16)
$${\text{MgCa}}\left( {{\text{CO}}_{3} } \right)_{2} + {\text{H}}^{ + } \to {\text{Mg}}^{2 + } + {\text{Ca}}^{2 + } + {\text{H}}_{2} {\text{O}} + {\text{CO}}_{2} \left( {\text{g}} \right)$$
(17)

In summary, the main changes in the mineral phase of the fallen rock are reflected in the dissolution of albite and orthoclase, precipitation of kaolinite, illite and quartz, and redox reaction between pyrite and siderite. The main actions of the underground reservoir in Daliuta Coal Mine are leaching, cation alternate adsorption and redox, which cause the water quality of the mine to change.

4 Conclusions

  1. (1)

    The groundwater reservoir of Daliuta Coal Mine is dominated by sandstone, accounting for 70%, and mudstone accounts for 30%. Due to its composition, it is closely arranged in the groundwater reservoir, which plays a key role in the purification of water in the underground reservoir. In sandstone, feldspar has the highest content, followed by clay, and contains a small amount of pyrite and augite; while in mudstone, clay has the highest content, followed by feldspar, and contains a small amount of chlorite.

  2. (2)

    Through simulation experiments, it is found that the underground reservoir of Daliuta Coal Mine mainly undergoes leaching, cation alternating adsorption, and redox. After the action of water–rock, the content of albite and orthoclase decreased, the content of kaolinite, illite, and quartz increased, and pyrite and siderite decreased slightly. Before and after the inflow of mine water, Na+, Cl− and HCO −3 increased, and Ca2+, Mg2+, and SO42− decreased. The results of the simulation experiments agree with the facts in the real mine. Water–rock interaction will lead to the change of mineral surface structure and pore distribution, which will affect the subsequent purification effect of mine water. The rock adsorption capacity gradually weakens with the action of water–rock. To improve the purification ability of groundwater quality water, the groundwater reservoir should be dredged regularly.