## 3 Results
### Thermodynamic Modeling Results  
As shown in Figure 9, when equilibrium at 2 \({}^{\circ}\)C is reached, a small amount of gypsum, dolomite, quartz, and hematite is precipitated from the solutions. Figure 8: Contour plots of temperature distribution in thawed rock (well t1) at different times. The simulation period is 10 years. The ambient rock temperature is +4 \({}^{\circ}\)C and the velocity of water flowing into the cylindrical channel is 100 m/day. A slightly modified chemical composition will enter the storage pond. With the temperature increase in the shunting tank storage pond only from the equilibration solution, i.e., without interaction with the sides of the tailing dump, only dolomite deposition is possible. The reactions are exothermic and when the solution is equilibrated, the temperature rises by 4.2 \({}^{\circ}\)C, irrespective of the initial temperature (initial values from 2 to 8 \({}^{\circ}\)C were estimated). Two scenarios mineral equilibria for limestones, tailings (psephites), and marks are shown in Figure 10, namely, \"dry rocks\" and equilibria after the addition of a 10% solution (A01). Figure 10: Equilibrium composition of the discussed rocks. Figure 9: Estimated mineral composition of sediments from the solution of the settling pond (A01). As shown, when reacting with a solution, the composition of the rocks changes, and the proportion of water-bearing minerals increases. The most significant changes occur in limestones; marks are also subject to a noticeable change in mineral composition. In addition, the reactions of the replacement minerals under exogenous conditions are much slower than primary minerals. Due to the increase in volume, the permeability of the rock decreases and natural seals are formed. In addition, minerals containing a hydroxyl group (i.e., OH\(-\)) have higher sorption capabilities as an example--the formation of illite, chlorite due to the transformation of primary silicates, gypsum instead of anhydrite, an increase in the proportion of dolomite due to the destruction of Mg-containing minerals. Notably, there is no specific formula for calculating the degree of rock transformation; this phenomenon instead depends on many factors including temperature, pressure, fluid flow, interaction surface, etc. According to changes in bicarbonate ions in the solutions, we estimated that 0.0001% of limestone would react if the rock composition of the entire dam massif is taken into account. If we consider the reactions of water-rock interaction in the predicted bypass filtration zones, then, according to our estimates, 0.01% of limestone would undergo the dissolution processes. First, we considered the possibility of exogenous reactions increasing the temperature due to chemical reactions during the equilibration of solutions. The temperature changes (\(\Delta\)T \({}^{\circ}\)C) were calculated for the rocks, assuming that 0.01% of the rock mass entered into reactions with a solution. When comparing the heat released during the interaction of solutions with tailings, marks, and limestones, we calculated that the maximum heat release occurs with limestone. In addition, based on field observations in the study area, limestones are the most susceptible lithology to weathering by the modern anthropogenic processes occurring in the tailing dump. The temperature changes during the dissolution reactions of 0.00001-0.12% limestone were also calculated. In the range from 0.00001% to 0.001% limestone dissolution, the temperature change is determined only by the solution equilibration reaction and reaches a value of 4.2 \({}^{\circ}\)C. If 0.01% of the mass of limestone dissolves, the contribution from changes in the limestone reaches 2.6 \({}^{\circ}\)C. Based on the field observations, it can be assumed with a high degree of certainty that between 0.01 and 0.1% of the rocks are currently reacting, therefore, more detailed calculations were carried out for this interval of the solution/rock ratio.