Method for analyzing hydrological characteristics of a metal deposit

Abstract

This invention relates to the field of hydrological analysis technology, specifically disclosing a method for analyzing the hydrological characteristics of metal deposits. The method includes: at multiple sampling points within the mining area of ​​the metal deposit, projecting the major ion concentration of each water sample onto a pre-defined Piper triangular diagram of cations and anions, and connecting the coordinates of the cation phase diagram and the anion phase diagram generated for each water sample to form the topological edges of the hydrochemical phase diagram of the metal deposit; determining the initial water source type of the water sample based on the topological similarity between the topological edges of the hydrochemical phase diagrams of various pre-defined standard water sources and the topological edges of the hydrochemical phase diagrams; calculating the water-rock interaction activity index based on the rate of change of the basic hydrochemical parameters of the water sample over time, relative to the deviation of the standard mineral dissolution equilibrium constant corresponding to the initial water source type, to dynamically assess the risk status of the water inflow channel of the metal deposit; this invention can improve the efficiency of hydrological characteristic analysis of metal deposits.

Description

Technical Field

[0001] This invention relates to the field of hydrological analysis technology, and in particular to a method for analyzing the hydrological characteristics of metal deposits. Background Technology

[0002] Current analyses of the hydrological characteristics of metal deposits largely rely on single physical hydrodynamic parameters or simple comparisons of hydrochemical ion concentrations. These methods only focus on water level changes or exceeding the limits of a single ion concentration threshold, failing to systematically analyze the synergistic relationships between multiple components of hydrochemical characteristics. Consequently, when faced with water bodies from different sources such as roof water, tectonic fracture water, and old workings water, it is difficult to accurately distinguish the differences in hydrochemical fingerprints of each water source, resulting in low accuracy and reliability in water source identification.

[0003] Furthermore, existing technologies generally lack a technical correlation between the dynamic evolution characteristics of hydrochemistry and the development status of water-conducting channels. Mining disturbances continuously intensify water-rock interactions, causing hydrochemical parameters to exhibit dynamic changes. However, traditional methods only perform isolated analyses of static water samples, failing to establish an evaluation system for the deviation between the rate of change in ion proportions and the mineral dissolution equilibrium constant. This makes it impossible to map the temporal evolution characteristics of hydrochemical information to the activation risk level of water-conducting channels, thus hindering dynamic early warning of water inrush risks in metal deposits. Summary of the Invention

[0004] In view of the above problems, the purpose of this invention is to provide a method for analyzing the hydrological characteristics of metal deposits, so as to solve the problems that existing methods for analyzing the hydrological characteristics of metal deposits have low accuracy in distinguishing water bodies from different sources due to the lack of collaborative analysis of multi-component hydrochemical characteristics, and cannot achieve dynamic early warning of the risk of activation of water conduits under mining disturbances because they have not established a technical correlation between the dynamic evolution characteristics of hydrochemistry and the development status of water-conducting channels.

[0005] This invention provides a method for analyzing the hydrological characteristics of metal deposits, comprising: Step 1: At multiple sampling points within the mining area of ​​the metal deposit, project the main ion concentration of each water sample onto the cation and anion triangular diagram of the preset Piper triangular diagram, and connect the coordinates of the cation phase diagram and the anion phase diagram of each water sample to form the topological edge of the hydrochemical phase diagram of the metal deposit. Step 2: Determine the initial water source type of the water sample based on the topological similarity between the topological edges of the water chemical phase diagram of various preset standard water sources and the topological edges of the water chemical phase diagram; Step 3: Based on the rate of change of the basic hydrochemical parameters of the water sample over time and the degree of deviation from the standard mineral dissolution equilibrium constant corresponding to the initial water source type, calculate the water-rock interaction activity index to dynamically assess the risk status of the water inflow channel of the metal deposit.

[0006] Preferably, the process of projecting the major ion concentration of each water sample onto the cation and anion triangle of a preset Piper triangular diagram is as follows: After normalizing the concentration values ​​of sodium, potassium, calcium, and magnesium ions in each water sample, they are mapped to the coordinates of the inner points of the cation triangle diagram in the preset Piper triangular diagram to generate the cation phase diagram coordinates of each water sample. After normalizing the concentration values ​​of chloride ions, sulfate ions, and bicarbonate ions in each water sample, they are mapped to the corresponding coordinate points of the anion triangular diagram in the Piper triangular diagram to generate the anion phase diagram coordinates of each water sample.

[0007] Preferably, the process of generating the cation phase diagram coordinates for each water sample is as follows: The total cations are the sum of the concentrations of sodium, potassium, calcium, and magnesium ions in the water sample, and the normalized concentration is the ratio of the concentration of each ion to the total cations. Based on the definition of the interior point coordinates of the cation triangle in the Piper triangular diagram, the normalized concentration values ​​are respectively assigned as the weighting coefficients of the interior point coordinates in the directions of the three vertices in the cation triangle. Based on the weighting coefficients, the concentrations of each ion in each water sample are weighted and averaged to obtain the cation phase diagram coordinates of each water sample.

[0008] Preferably, the process of connecting the cation phase diagram coordinates and anion phase diagram coordinates generated from each water sample to form the topological edge of the hydrochemical phase diagram of the metal deposit is as follows: Using the central rhomboid region of the Piper tri-line diagram as the connecting plane, and taking the coordinates of the cation phase diagram belonging to the same water sample as the starting point and the coordinates of the anion phase diagram as the ending point, draw straight line segments within the central rhomboid region; The straight line segment is used as the topological edge of the hydrochemical phase diagram of the water sample.

[0009] Preferably, the process of determining the initial water source type of the water sample based on the topological similarity between the topological edges of the hydrochemical phase diagrams of various preset standard water sources and the topological edges of the hydrochemical phase diagrams is as follows: The preset standard water sources include the standard topological edges of roof water sources, structural fissure water sources, and old void water sources. Calculate the Fraser distance between the topological edges of the hydrochemical phase diagram of the water sample and various standard topological edges, and determine the water source type corresponding to the standard topological edge with the smallest Fraser distance as the initial water source type of the water sample.

[0010] Preferably, the process of calculating the Fréchet distances between the topological edges of the water sample's hydrochemical phase diagram and the preset standard water sources is as follows: Within the central rhomboid region of the Piper trilinear diagram, the topological edges of the hydrochemical phase diagram of the water sample and each of the standard topological edges are discretely sampled with the same preset arc length step size to obtain the first discrete point sequence of the water sample and the second discrete point sequence of each of the standard topological edges. Calculate the Euclidean distance between each discrete point pair between the first discrete point sequence and each of the second discrete point sequences; The minimum value of the supremum among all Euclidean distances is taken as the Fraser distance between the topological edge of the water sample's hydrochemical phase diagram and the preset standard water sources.

[0011] Preferably, the rate of change of the basic hydrochemical parameters of the water sample over time is as follows: According to the equal time sampling period, water samples are continuously taken from each sampling point in the metal deposit, and the water temperature, conductivity, pH, total dissolved solids and content of major and minor ionic components of each group of water samples are measured simultaneously to form the basic hydrochemical parameters of the water samples. The basic hydrochemical parameters of the water sample are fitted with nonlinear trends, and the obtained gradual change rate and fluctuation change rate are combined to form the comprehensive time change rate of the basic hydrochemical parameters.

[0012] Preferably, the process of calculating the water-rock interaction activity index based on the degree of deviation from the standard mineral dissolution equilibrium constant corresponding to the initial water source type is as follows: Based on the comprehensive time change rate of each basic hydrochemical parameter, the water-rock reaction process between groundwater and surrounding rock minerals in the metal deposit is inverted to obtain the actual mineral dissolution equilibrium constant of the metal deposit. Based on the standard mineral dissolution equilibrium constant spectrum under the mineral system corresponding to the initial water source type, and the multi-dimensional comparison results between the actual mineral dissolution equilibrium constant, the water-rock interaction activity index of the metal deposit is calculated.

[0013] Preferably, the water-rock interaction activity index of the metal deposit is determined as follows: The multi-dimensional comparison results include the deviation of ion group distribution ratio, the deviation of concentration time decay, and the deviation of acid-base buffering capacity; Based on the stratigraphic lithology, structural fragmentation, and groundwater runoff conditions of the metal deposit, corresponding geological constraint weights are assigned to the three types of characteristic deviations. Based on the geological constraint weights, the water-rock interaction activity index of the metal deposit is calculated, wherein the calculation formula for the water-rock interaction activity index is as follows: ; In the formula, This represents the water-rock interaction activity index. This indicates the deviation of the ion group distribution ratio. This represents the geological constraint weight corresponding to the deviation of the ion group distribution ratio. This indicates the deviation of the concentration from the time-series decay. This represents the geological constraint weight corresponding to the concentration time-series decay deviation. This indicates the deviation of the acid-base buffering capacity. This represents the geological constraint weight corresponding to the deviation of the acid-base buffering capacity. This represents the preset water source topology difference correction coefficient. This represents the Fraser distance between the topological edges of the current water sample's hydrochemical phase diagram and the preset standard water sources. This represents the minimum Fraser distance among all sampling points in the metal deposit. This represents the maximum value of the Fraser distance among all sampling points in the metal deposit.

[0014] Preferably, the process of dynamically assessing the risk status of the water inflow channels of the metal deposit is as follows: Based on historical water inrush cases of the metal deposit, the critical values ​​of the first and second thresholds are graded and calibrated. When the water-rock interaction activity index is between the benchmark value and the first threshold, the water-conducting channel of the metal deposit is determined to be in a stable and normal state. When the water-rock interaction activity index exceeds the first threshold but does not reach the second threshold, it is determined that the water-conducting channel fractures of the metal deposit are expanding and the degree of activation is continuously intensifying. When the water-rock interaction activity index exceeds the second threshold, it is determined that the surrounding rock fissures of the metal deposit are connected and the water-conducting channels are unstable, posing a risk of water inrush in the roadway or working face.

[0015] As can be seen from the above technical solution, the present invention provides a method for analyzing the hydrological characteristics of metal deposits. By constructing the topological edges of the hydrochemical phase diagram of water samples and calculating the topological similarity between them and the topological edges of various standard water sources, it achieves accurate identification of water bodies from different sources in metal deposits, overcoming the problem of low accuracy of traditional single ion concentration comparison methods. At the same time, based on the deviation of the rate of change of basic hydrochemical parameters over time from the dissolution equilibrium constant of the standard minerals corresponding to the initial water source type, the present invention calculates the water-rock interaction activity index, quantifies the hydrochemical time-series evolution characteristics into the risk level of water inflow channels, and realizes dynamic monitoring and risk warning of the activation state of water-conducting channels under mining disturbance, significantly improving the comprehensiveness and timeliness of hydrological characteristic analysis of metal deposits. Attached Figure Description

[0016] Other objects and results of the invention will become more apparent and readily understood by referring to the following description taken in conjunction with the accompanying drawings, and with a more complete understanding of the invention. In the drawings: Figure 1 This is a flowchart illustrating a method for analyzing the hydrological characteristics of a metal deposit according to an embodiment of the present invention. Detailed Implementation

[0017] Existing methods for analyzing the hydrological characteristics of metal deposits lack the ability to perform synergistic analysis of the hydrochemical characteristics of multiple components, resulting in low accuracy in distinguishing water bodies from different sources. Furthermore, the lack of a technical correlation between the dynamic evolution characteristics of hydrochemistry and the development status of water-conducting channels prevents dynamic early warning of the risk of activation of water-conducting channels under mining disturbances.

[0018] To address the aforementioned problems, this invention provides a method for analyzing the hydrological characteristics of metal deposits. The specific embodiments of this invention will be described in detail below with reference to the accompanying drawings.

[0019] To illustrate the method for analyzing the hydrological characteristics of metal deposits provided by this invention Figure 1 An exemplary illustration is provided for a method for analyzing the hydrological characteristics of a metal deposit according to an embodiment of the present invention.

[0020] The following description of exemplary embodiments is merely illustrative and is in no way intended to limit the invention or its application or use. Techniques and equipment known to those skilled in the art may not be discussed in detail, but where appropriate, such techniques and equipment should be considered part of the specification.

[0021] Reference Figure 1 The diagram shown is a flowchart illustrating a method for analyzing the hydrological characteristics of a metal deposit according to an embodiment of the present invention. In this embodiment, the method for analyzing the hydrological characteristics of a metal deposit includes: Step 1: At multiple sampling points within the mining area of ​​the metal deposit, project the main ion concentration of each water sample onto the cation and anion triangular diagram of the preset Piper triangular diagram, and connect the coordinates of the cation phase diagram and the anion phase diagram of each water sample to form the topological edge of the hydrochemical phase diagram of the metal deposit. In this embodiment of the invention, the process of projecting the major ion concentration of each water sample onto the cation and anion triangle diagram of a preset Piper triangular plot is as follows: After normalizing the concentration values ​​of sodium, potassium, calcium, and magnesium ions in each water sample, they are mapped to the coordinates of the inner points of the cation triangle diagram in the preset Piper triangular diagram to generate the cation phase diagram coordinates of each water sample. After normalizing the concentration values ​​of chloride ions, sulfate ions, and bicarbonate ions in each water sample, they are mapped to the corresponding coordinate points of the anion triangular diagram in the Piper triangular diagram to generate the anion phase diagram coordinates of each water sample.

[0022] The process of generating the cation phase diagram coordinates for each water sample is as follows: The total cations are the sum of the concentrations of sodium, potassium, calcium, and magnesium ions in the water sample, and the normalized concentration is the ratio of the concentration of each ion to the total cations. Based on the definition of the interior point coordinates of the cation triangle in the Piper triangular diagram, the normalized concentration values ​​are respectively assigned as the weighting coefficients of the interior point coordinates in the directions of the three vertices in the cation triangle. Based on the weighting coefficients, the concentrations of each ion in each water sample are weighted and averaged to obtain the cation phase diagram coordinates of each water sample.

[0023] The process of connecting the coordinates of the cation phase diagram and the coordinates of the anion phase diagram generated from each water sample to form the topological edge of the hydrochemical phase diagram of the metal deposit is as follows: Using the central rhomboid region of the Piper tri-line diagram as the connecting plane, and taking the coordinates of the cation phase diagram belonging to the same water sample as the starting point and the coordinates of the anion phase diagram as the ending point, draw straight line segments within the central rhomboid region; The straight line segment is used as the topological edge of the hydrochemical phase diagram of the water sample.

[0024] Water samples were collected from multiple sampling points within the mining area of ​​the metal deposit. Chemical analysis was performed on each sample to obtain the concentrations of sodium, potassium, calcium, and magnesium ions. These concentrations were then summed; the total sum of these concentrations represents the total cations in the water sample. The normalized concentrations of sodium, potassium, calcium, and magnesium ions were obtained by dividing the sodium concentration by the total cations, the same applies to calcium and magnesium ions. These normalized concentrations represent the proportion of each ion in the total cations.

[0025] The cation triangle diagram in the Piper triangular plot has three vertices: the first vertex corresponds to the direction of sodium and potassium ions, the second to calcium ions, and the third to magnesium ions. The interior point coordinates are defined as the contribution of each vertex direction to the point's position. The normalized concentration values ​​of sodium and potassium ions in each water sample are added together to obtain the combined normalized concentration value of sodium and potassium ions. This value serves as the weighting coefficient for the interior point coordinates in the direction of the sodium and potassium ion vertex. The normalized concentration value of calcium ions is used as the weighting coefficient for the calcium ion vertex direction. The normalized concentration value of magnesium ions is used as the weighting coefficient for the magnesium ion vertex direction. In this way, the normalized concentration values ​​of each water sample are converted into weighting coefficients for the interior point coordinates in the three vertices of the cation triangle diagram.

[0026] The three vertices of the cation phase diagram have fixed positions in the coordinate system: the sodium and potassium ion vertices have fixed coordinates, the calcium ion vertices have fixed coordinates, and the magnesium ion vertices have fixed coordinates. For each water sample, the weighting coefficients of the sodium and potassium ion vertices are multiplied by the coordinates of their respective vertices to obtain the first product. The weighting coefficient of the calcium ion vertices is multiplied by the coordinates of its respective vertex to obtain the second product. The weighting coefficient of the magnesium ion vertices is multiplied by the coordinates of its respective vertex to obtain the third product. The first, second, and third products are added together to obtain the cation phase diagram coordinates for that water sample. These coordinates represent a point within the cation phase diagram.

[0027] The concentrations of chloride, sulfate, and bicarbonate ions in each water sample were normalized. The sum of the chloride, sulfate, and bicarbonate ion concentrations was calculated as the total anion concentration. The normalized chloride concentration was obtained by dividing the chloride concentration by the total anion concentration. The normalized sulfate concentration was obtained by dividing the sulfate concentration by the total anion concentration. The normalized bicarbonate concentration was obtained by dividing the bicarbonate concentration by the total anion concentration. The Piper triangular diagram of anions has three vertices: the first vertex corresponds to the direction of chloride ions, the second to the direction of sulfate ions, and the third to the direction of bicarbonate ions. Each vertex has fixed coordinates. The normalized chloride concentration was mapped to the coordinates of the chloride vertex, the sulfate concentration to the coordinates of the sulfate vertex, and the bicarbonate concentration to the coordinates of the bicarbonate vertex. These three normalized concentration values ​​were used to determine a point in the anion triangular diagram; this point is the anion phase diagram coordinate for that water sample.

[0028] The central rhombus region of the Piper triangular plot is formed by combining cation and anion triangular plots. For each water sample, its cation phase diagram coordinates are used as the starting point, and its anion phase diagram coordinates as the ending point. In the coordinate system of the central rhombus region, a straight line segment is drawn from the starting point coordinates to the ending point coordinates using a drawing tool. This straight line segment connects the starting and ending points and lies entirely within the central rhombus region. When drawing, ensure that the straight line segment accurately reflects the positions of the starting and ending points.

[0029] The straight line segment drawn for each water sample within the central rhombus region is defined as the topological edge of the hydrochemical phase diagram for that water sample. The set of straight line segments from all water samples constitutes the topological edge of the hydrochemical phase diagram of the metallic deposit. These topological edges, displayed in the Piper triline diagram, illustrate the spatial distribution and interrelationships of the ionic composition of the water samples.

[0030] Step 2: Determine the initial water source type of the water sample based on the topological similarity between the topological edges of the water chemical phase diagram of various preset standard water sources and the topological edges of the water chemical phase diagram; In this embodiment of the invention, the process of determining the initial water source type of the water sample based on the topological similarity between the topological edges of the hydrochemical phase diagrams of various preset standard water sources and the topological edges of the hydrochemical phase diagrams is as follows: The preset standard water sources include the standard topological edges of roof water sources, structural fissure water sources, and old void water sources. Calculate the Fraser distance between the topological edges of the hydrochemical phase diagram of the water sample and various standard topological edges, and determine the water source type corresponding to the standard topological edge with the smallest Fraser distance as the initial water source type of the water sample.

[0031] The process of calculating the Fréchet distances between the topological edges of the hydrochemical phase diagram of the water sample and the preset standard water sources is as follows: Within the central rhomboid region of the Piper trilinear diagram, the topological edges of the hydrochemical phase diagram of the water sample and each of the standard topological edges are discretely sampled with the same preset arc length step size to obtain the first discrete point sequence of the water sample and the second discrete point sequence of each of the standard topological edges. Calculate the Euclidean distance between each discrete point pair between the first discrete point sequence and each of the second discrete point sequences; The minimum value of the supremum among all Euclidean distances is taken as the Fraser distance between the topological edge of the water sample's hydrochemical phase diagram and the preset standard water sources.

[0032] Before conducting water source identification, a benchmark reference system for comparison must first be established. This reference system consists of the topological edges of the hydrochemical phase diagrams of various standard water sources, specifically including the standard topological edges of roof water sources, structural fissure water sources, and old void water sources. The establishment of each standard topological edge is based on a large amount of ion concentration data from historical water samples. By drawing the topological edges of representative water samples of each known water source type in the central diamond area of ​​the Piper triline diagram, and summarizing their shape and location characteristics, a statistically representative average curve or typical curve is derived. This curve is established as the standard topological edge of that type of water source, which serves as an immutable template in subsequent comparisons.

[0033] Within the coordinate system of the central rhomboid region of the Piper trilinear diagram, discretization data is collected for the topological edges of the hydrochemical phase diagram generated for the unknown water sample to be identified. This process uses a pre-set fixed arc length step size. Starting from the starting point of the topological edge, the arc length is continuously measured along the curve using this step size. At each step size, the planar coordinates of the point at the corresponding position on the curve are recorded until the end point of the topological edge is reached. All the coordinate points recorded in this way constitute the first discrete point sequence representing the shape of the topological edge of the water sample. Then, using the exact same preset arc length step size, the above discrete sampling process is repeated independently for each preset standard topological edge. For example, the second discrete point sequence is obtained by sampling the standard topological edge of the roof water source, the second discrete point sequence is obtained by sampling the standard topological edge of the tectonic fissure water source, and the second discrete point sequence is obtained by sampling the standard topological edge of the old void water source. Thus, a corresponding second discrete point sequence is generated for each type of standard water source to characterize the shape of its standard curve.

[0034] Then, the first discrete point sequence of the unknown water sample is sequentially compared with the second discrete point sequence of each standard water source, and the distance between each point is calculated. Taking the comparison with the standard topological edge of the top plate water source as an example, the first point in the first discrete point sequence is paired with the first point in the second discrete point sequence of the top plate water source, and the straight-line distance between these two points, i.e., the Euclidean distance, is calculated. The calculation method is to take the difference between the x-coordinate and the y-coordinate of the two points, square these two differences respectively, add them together, and then take the square root of the sum to obtain the Euclidean distance of the first point pair. Next, the second point of the first sequence is paired with the second point of the second sequence, and the Euclidean distance of the second point pair is calculated in the same way. This process is repeated to calculate the Euclidean distance between all corresponding point pairs in sequence. Finally, a set of Euclidean distances containing the distance values ​​of all point pairs is obtained. This set describes the deviation between the water sample curve and the current standard curve at the corresponding point positions.

[0035] After obtaining all point-to-point Euclidean distances between the water sample and a certain type of standard water source, the largest value is found from this set of Euclidean distance values. This maximum value is mathematically defined as the supremum of the distance set, which represents the maximum deviation between the water sample curve and the standard curve at all corresponding points. Then, the above calculation is performed for each type of standard water source to obtain the supremum of the water sample curve with the topological edge of the roof water source standard, the supremum of the water sample curve with the topological edge of the tectonic fracture water source standard, and the supremum of the water sample curve with the topological edge of the old void water source standard. Then, from these three specific supremum values, the smallest value is selected. The physical meaning of this selected minimum value is the minimum of the maximum deviations that the unknown water sample curve needs to overcome compared with all standard curves. It is formally defined as the Fraser distance between the topological edge of the water sample's hydrochemical phase diagram and the preset types of standard water sources. The Fraser distance is a holistic index used to measure the similarity between two curves.

[0036] The final step is to determine the water source type based on the Fraser distance. All calculated Fraser distance values ​​are compared, and the smallest value is identified. This smallest value is then determined by comparing it to the topological edge of a standard water source. The water source type represented by that standard topological edge is then identified as the initial water source type of the unknown water sample. For example, if the Fraser distance calculated with the standard topological edge of a roof water source is the smallest of the three values, then the initial water source type of the water sample is determined to be roof water. This determination process is based on the principle of the most similar overall curve shape.

[0037] Step 3: Based on the rate of change of the basic hydrochemical parameters of the water sample over time and the degree of deviation from the standard mineral dissolution equilibrium constant corresponding to the initial water source type, calculate the water-rock interaction activity index to dynamically assess the risk status of the water inflow channel of the metal deposit.

[0038] In this embodiment of the invention, the rate of change of the basic water chemical parameters of the water sample over time is as follows: According to the equal time sampling period, water samples are continuously taken from each sampling point in the metal deposit, and the water temperature, conductivity, pH, total dissolved solids and content of major and minor ionic components of each group of water samples are measured simultaneously to form the basic hydrochemical parameters of the water samples. The basic hydrochemical parameters of the water sample are fitted with nonlinear trends, and the obtained gradual change rate and fluctuation change rate are combined to form the comprehensive time change rate of the basic hydrochemical parameters.

[0039] The degree of deviation from the standard mineral dissolution equilibrium constant corresponding to the initial water source type is used to calculate the water-rock interaction activity index, and the process is as follows: Based on the comprehensive time change rate of each basic hydrochemical parameter, the water-rock reaction process between groundwater and surrounding rock minerals in the metal deposit is inverted to obtain the actual mineral dissolution equilibrium constant of the metal deposit. Based on the standard mineral dissolution equilibrium constant spectrum under the mineral system corresponding to the initial water source type, and the multi-dimensional comparison results between the actual mineral dissolution equilibrium constant, the water-rock interaction activity index of the metal deposit is calculated.

[0040] The water-rock interaction activity index of the metal deposit is determined as follows: The multi-dimensional comparison results include the deviation of ion group distribution ratio, the deviation of concentration time decay, and the deviation of acid-base buffering capacity; Based on the stratigraphic lithology, structural fragmentation, and groundwater runoff conditions of the metal deposit, corresponding geological constraint weights are assigned to the three types of characteristic deviations. Based on the geological constraint weights, the water-rock interaction activity index of the metal deposit is calculated, wherein the calculation formula for the water-rock interaction activity index is as follows: ; In the formula, This represents the water-rock interaction activity index. This indicates the deviation of the ion group distribution ratio. This represents the geological constraint weight corresponding to the deviation of the ion group distribution ratio. This indicates the deviation of the concentration from the time-series decay. This represents the geological constraint weight corresponding to the concentration time-series decay deviation. This indicates the deviation of the acid-base buffering capacity. This represents the geological constraint weight corresponding to the deviation of the acid-base buffering capacity. This represents the preset water source topology difference correction coefficient. This represents the Fraser distance between the topological edges of the current water sample's hydrochemical phase diagram and the preset standard water sources. This represents the minimum Fraser distance among all sampling points in the metal deposit. This represents the maximum value of the Fraser distance among all sampling points in the metal deposit.

[0041] The deviation of the ion component distribution ratio originates from the calculation of the concentration ratio of the main cations and anions in the water sample. The specific method involves first converting the measured concentrations of calcium, magnesium, sodium, potassium, bicarbonate, sulfate, and chloride ions in the water sample into stoichiometric concentrations. Then, the stoichiometric ratios between cations and between anions are calculated separately. These calculated ion ratios are then compared one by one with the stoichiometric ratios of standard water corresponding to the initial water source type of the water sample, and the numerical differences in these ratios are determined. All differences in ion ratios are then averaged or summed to obtain the final numerical value, which is the deviation of the ion component distribution ratio.

[0042] The concentration-time decay deviation originates from the analysis of the rate of change of a specific ion concentration over time. Specifically, the method involves retrieving a long-term, continuous monitoring data series of a specific indicative ion concentration from the sampling point's history. Using a nonlinear trend fitting method, short-term random fluctuations are eliminated, revealing the overall gradual rate of change of the ion concentration over time. Subsequently, this measured gradual rate of change is compared with the expected, stable theoretical ion decay or enrichment rate for this type of water source under standard hydrogeological conditions, and the difference between the two is calculated. The magnitude of this difference directly reflects the degree of deviation of the groundwater ion concentration change from the standard state; this specific value is the concentration-time decay deviation.

[0043] The deviation of acid-base buffering capacity originates from the determination of a water sample's ability to resist changes in acidity and alkalinity. The specific method involves obtaining the pH value of the water sample through laboratory or field measurements, and combining this with the concentrations of acidic and alkaline components such as carbonic acid, bicarbonate, and carbon dioxide. A specific acid-base balance model is then used to calculate the actual acid-base buffering capacity of the water sample. This actual buffering capacity is compared with the standard buffering capacity that this type of water source in the metal deposit should possess under normal conditions, and the difference between the two is calculated. The specific value of this difference is the deviation of the acid-base buffering capacity, which quantifies the degree of disturbance to the acid-base environment of the water body caused by the current water-rock reaction.

[0044] The Fraser distance is derived from a similarity measure of the geometric shape of the topological edges of the hydrochemical phase diagram. Specifically, within the central diamond region of the Piper trilinear diagram, the topological edges of the hydrochemical phase diagram drawn from the current water sample, as well as the standard topological edges of pre-defined top-plate water sources, tectonic fissure water sources, and old void water sources, are transformed into a series of polylines composed of dense coordinate points. Using a specific curve similarity matching algorithm, the Fraser distance between the current water sample's topological edge and each standard topological edge is calculated one by one. During the calculation, the optimal pairing of corresponding points between two polylines is sought, minimizing the total length of the line connecting the corresponding points. This minimum total length is the specific value of the Fraser distance, representing the maximum difference in overall shape and trend between the current water sample curve and the standard curve.

[0045] The minimum and maximum values ​​of the Fraser distance are derived from a full scan of the monitoring network's data. Specifically, this involves traversing all sampling points within the metal deposit, extracting the Fraser distance data calculated and saved for each point in historical monitoring, and then filtering for extreme values ​​within this dataset. The smallest value among all values ​​is defined as the minimum Fraser distance; the largest value is defined as the maximum Fraser distance. These two extreme values ​​together construct a global reference range for the hydrochemical topological characteristics of the deposit.

[0046] The geological constraint weights are derived from a professional assessment of the dominant factors in water-rock reactions under different geological conditions. Specifically, this involves a detailed analysis of the geological background of the target metal deposit, including stratigraphic lithology, tectonic fracturing, and groundwater runoff conditions. Based on the expertise and long-term practical experience of hydrogeologists, it is determined whether, under the specific geological background, changes in ion proportions, concentration decay rates, or acid-base buffering capacity have a decisive indicative significance for the intensity of water-rock interactions. Parameters with greater indicative significance and better reflect the nature of water-rock reactions under the current geological environment are assigned higher importance values; relatively less important parameters are assigned lower values. Through this weighting process, the specific geological constraint weights corresponding to the deviations in ion composition ratios, concentration temporal decay, and acid-base buffering capacity are ultimately determined.

[0047] The source topology difference correction coefficient is derived from a priori assumptions about the spatial variability of hydrochemical characteristics. Specifically, it involves comprehensively considering the complexity of hydrogeological conditions in different sections of the metal deposit, the dispersion of hydrochemical monitoring data, and the potential topological distortions caused by water mixing. Based on a comprehensive consideration of these potential influencing factors, a fixed empirical value is pre-set. This value is used to amplify or reduce the topological shape differences reflected by the Fraser distance in the calculation of water-rock interaction activity, ensuring that the final activity index more accurately reflects the actual geochemical evolution patterns on site. This pre-set fixed value is the source topology difference correction coefficient.

[0048] The overall significance of the formula lies in constructing a comprehensive quantitative evaluation model to accurately characterize the intensity of the interaction between groundwater and surrounding rocks in metal deposits. It integrates the three-dimensional deviation information of hydrochemical ion characteristics, the geometric differences in the topological morphology of hydrochemical phase diagrams, and the importance of specific geological backgrounds on each indicator into a unified mathematical framework for quantitative expression. Through this model, complex, multi-dimensional hydrogeochemical monitoring data can be transformed into a single, clearly physically meaningful comprehensive index—the water-rock interaction activity index. The core value of this index lies in breaking the limitations of single-indicator evaluation, providing a quantitative benchmark that comprehensively and objectively reflects the overall intensity of water-rock reactions, and providing solid data support and theoretical basis for subsequent assessments of the stability of water-conducting channels.

[0049] The formula shows a clear positive correlation between the water-rock interaction activity index and the various input parameters. When the deviation of the ion composition ratio in the water sample increases, it indicates that the water-rock reaction is significantly altering the chemical composition of the groundwater, directly leading to a linear increase in the calculated water-rock interaction activity index. When the deviation of the concentration decay over time increases, it indicates that the rate of change in ion concentration over time exceeds the normal background level, reflecting an accelerated mineral dissolution or precipitation reaction, which in turn directly leads to an increase in the calculated water-rock interaction activity index. When the deviation of the acid-base buffering capacity increases, it indicates that the water-rock reaction has caused a severe disturbance to the acid-base balance of the water body, which also leads to an increase in the calculated water-rock interaction activity index. When the correction coefficient for water source topology difference increases, it indicates a greater emphasis on the differences in phase diagram topology between the current water sample and the standard water source, which amplifies the impact of topological differences, thus increasing the calculated water-rock interaction activity index. When the Fraser distance increases relative to the global minimum or decreases relative to the global maximum, it indicates a greater difference between the current water sample's topological edge and the most similar standard water source, reflecting a change in the hydrochemical evolution path. This increase in the normalized value also leads to a corresponding increase in the calculated water-rock interaction activity index. In summary, the water-rock interaction activity index is the result of the superposition of all positive driving factors. A larger value indicates more intense water-rock interactions, a greater deviation of the system from its initial equilibrium state, and a higher risk of activation or instability of the water-conducting channels.

[0050] The process of dynamically assessing the risk status of the water inflow channels in the metal deposit is as follows: Based on historical water inrush cases of the metal deposit, the critical values ​​of the first and second thresholds are graded and calibrated. When the water-rock interaction activity index is between the benchmark value and the first threshold, the water-conducting channel of the metal deposit is determined to be in a stable and normal state. When the water-rock interaction activity index exceeds the first threshold but does not reach the second threshold, it is determined that the water-conducting channel fractures of the metal deposit are expanding and the degree of activation is continuously intensifying. When the water-rock interaction activity index exceeds the second threshold, it is determined that the surrounding rock fissures of the metal deposit are connected and the water-conducting channels are unstable, posing a risk of water inrush in the roadway or working face.

[0051] At pre-defined sampling points within the metal deposit, groundwater samples are collected periodically at the same fixed time intervals. This interval can be daily, weekly, or monthly. At each sampling time, the water temperature is directly measured using a calibrated temperature probe, the conductivity is measured using a conductivity meter, the pH is measured using a pH meter, and the total dissolved solids (TDS) is determined using a total dissolved solids analyzer or by evaporation-drying and weighing. Simultaneously, the collected water samples are sent to a laboratory where standard methods such as ion chromatography or inductively coupled plasma mass spectrometry are used to accurately determine the specific contents of major and minor ions such as sodium, potassium, calcium, magnesium, chloride, sulfate, and bicarbonate ions. All these data on water temperature, conductivity, pH, TDS, and various ion contents obtained at the same time constitute the basic hydrochemical parameters of the water sample corresponding to that sampling. Over a long period of time, these data are accumulated to form a data sequence arranged in chronological order.

[0052] For each sampling point, a specific nonlinear mathematical fitting method is used to obtain a time-varying sequence of each basic water chemistry parameter, such as a series of data points showing the change of calcium ion concentration over time. Specifically, a curve model that can describe trend changes and fluctuations is selected, and the coefficients in the model are adjusted through iterative calculations to minimize the overall deviation of the curve from all time-series data points, thus obtaining an optimal fitting trend line that runs through the data points. From this trend line, the change in parameter value within any time period can be calculated and divided by time to obtain the time-series gradual change rate. At the same time, the standard deviation or mean absolute deviation of the difference between the original data points and the fitted trend line is calculated to measure the fluctuation amplitude of the data around the trend line, obtaining the fluctuation abrupt change rate. Finally, the absolute value of the time-series gradual change rate and the fluctuation abrupt change rate are multiplied by an appropriate coefficient and added together to generate a single, comprehensive index. This index is the comprehensive time change rate of the basic water chemistry parameter. Each parameter independently calculates its own comprehensive time change rate.

[0053] Based on the comprehensive time-varying rate of change calculated from all basic hydrochemical parameters, especially the concentration changes of ions directly involved in the water-rock reaction, such as calcium, magnesium, bicarbonate, and sulfate ions, as well as the changes in pH and conductivity, a reaction network model is constructed using the law of conservation of mass and the thermodynamic principle of mineral dissolution equilibrium. The observed ion concentration changes are then substituted into the model in reverse, and the reaction rates of each mineral in the model are adjusted through iterative calculations until the ion change trend calculated by the model best matches the measured comprehensive time-varying rate of change. This allows for the inversion of the specific rates and processes of dissolution or precipitation reactions between groundwater and minerals such as calcite, gypsum, and dolomite in the surrounding rock. Finally, a constant characterizing the current overall reaction equilibrium state of the system is obtained through inversion, which is the actual mineral dissolution equilibrium constant of the metal deposit.

[0054] Based on the initial water source type determined in the previous steps, such as old empty water, the pre-stored standard mineral dissolution equilibrium constant spectrum corresponding to this type of water source is retrieved. This spectrum contains the theoretical relationship between the concentrations of each ion when the water source reaches equilibrium with typical surrounding rock minerals under standard conditions. The actual mineral dissolution equilibrium constant obtained in the previous step is compared item by item with this standard spectrum. This multi-dimensional comparison result specifically produces three quantitative deviations: the first is the ion composition ratio deviation, which is obtained by calculating the average relative deviation between the ratio of the main anion and cation equivalent concentrations and the theoretical ratio in the standard spectrum; the second is the concentration time-series decay deviation, which is obtained by comparing the difference between the actual rate of decrease of the main ion concentration over time and the theoretical decay rate expected by the standard spectrum; the third is the acid-base buffering capacity deviation, which is obtained by comparing the difference between the change in pH of the actual water sample after the addition of standard acid or alkali and the theoretical buffering capacity corresponding to the standard spectrum.

[0055] Based on the specific geological characteristics of the deposit determined by the previous geological exploration report, borehole core logging, and groundwater dynamics test results, including the specific lithology and proportion of carbonate rocks and sandstones in the strata, the degree of structural fragmentation reflected by the density and opening of structures such as faults and joints, and the groundwater runoff velocity and direction obtained through tracer tests or water level observations, specific geological constraint weights are assigned to the above three deviations based on expert experience. For example, in carbonate rock strata with karst development, the deviation of ion composition ratio can sensitively reflect the dissolution process, so it is given a higher weight. In areas with high fragmentation, the concentration decay is faster, so the deviation of concentration decay is given a higher weight. In areas with slow groundwater runoff, acid-base conditions control the reaction, so the deviation of acid-base buffering capacity is given a higher weight. The specific values ​​of the weights are determined by expert scoring or analytic hierarchy process.

[0056] Based on the specific values ​​of the determined deviations in ion composition ratio, concentration-time decay, and acid-base buffering capacity, and the geological constraint weights assigned to them respectively, a weighted comprehensive calculation is performed. The specific calculation process is to multiply the value of the deviation in ion composition ratio by its corresponding geological constraint weight, the value of the deviation in concentration-time decay by its corresponding geological constraint weight, and the value of the deviation in acid-base buffering capacity by its corresponding geological constraint weight, and then add these three products together. The sum obtained is the water-rock interaction activity index of the metal deposit. This index is a dimensionless value that comprehensively quantifies the current intensity of water-rock interaction.

[0057] All recorded water inrush accident reports in the history of this metal deposit were collected. Hydrochemical monitoring data at different times before each water inrush were analyzed. The water-rock interaction activity index corresponding to each stage before the water inrush was calculated. Based on the suddenness of the water inrush, the size of the water inflow, and the severity of the consequences, the historical cases were divided into different risk levels, and two key threshold values ​​of the water-rock interaction activity index were marked. The lower threshold value is called the first threshold value, which usually corresponds to the inflection point when the water channel begins to show abnormal activity. The higher threshold value is called the second threshold value, which usually corresponds to the critical state when the channel is about to become unstable and water inrush is imminent.

[0058] When the calculated value of the current water-rock interaction activity index is higher than the baseline value obtained by the system under a long-term stable background, but lower than the first threshold, it is determined that the water-conducting channel of the current metal deposit is in a stable and normal state. This means that the groundwater flow path and surrounding rock structure have not changed significantly, and the hydrochemical dynamics are within the normal fluctuation range.

[0059] When the specific value of the water-rock interaction activity index is greater than the first threshold but has not yet reached the higher second threshold, it is determined that the water-conducting channel fracture network of the metal deposit is expanding, the permeability of the original fractures is increasing, new microfractures may be forming and connecting, the water-rock reaction rate is accelerating, and the system is deviating from the long-term stable state and developing in an unstable direction.

[0060] When the specific value of the water-rock interaction activity index exceeds the highest second threshold, it is determined that the surrounding rock fissures of the metal deposit have been fully connected under the combined action of hydraulic action and chemical dissolution to form a dominant water-conducting channel. The stability of the water-conducting structure is facing instability. At this time, the risk of large-scale, sudden water inrush in the roadway or working face is extremely high, and the highest level of early warning must be triggered immediately and the emergency response procedure must be initiated.

[0061] As can be seen from the above embodiments, the method for analyzing the hydrological characteristics of metal deposits provided by the present invention achieves accurate identification of water bodies from different sources in metal deposits by constructing the topological edges of the hydrochemical phase diagram of water samples and calculating the topological similarity between them and the topological edges of various standard water sources. This overcomes the problem of low accuracy of traditional single ion concentration comparison methods. At the same time, based on the deviation of the rate of change of basic hydrochemical parameters over time from the dissolution equilibrium constant of the standard minerals corresponding to the initial water source type, the present invention calculates the water-rock interaction activity index and quantifies the hydrochemical time-series evolution characteristics into the risk level of water inflow channels. This enables dynamic monitoring and risk warning of the activation state of water-conducting channels under mining disturbances, significantly improving the comprehensiveness and timeliness of the hydrological characteristic analysis of metal deposits.

[0062] It will be apparent to those skilled in the art that the present invention is not limited to the details of the exemplary embodiments described above, and that the present invention can be implemented in other specific forms without departing from the spirit or essential characteristics of the present invention.

[0063] Finally, it should be noted that the above embodiments are only used to illustrate the technical solutions of the present invention and are not intended to limit it. Although the present invention has been described in detail with reference to preferred embodiments, those skilled in the art should understand that modifications or equivalent substitutions can be made to the technical solutions of the present invention without departing from the spirit and scope of the technical solutions of the present invention.

Claims

1. A method for analyzing the hydrological characteristics of metal deposits, characterized in that, The method includes: Step 1: At multiple sampling points within the mining area of ​​the metal deposit, project the main ion concentration of each water sample onto the cation and anion triangular diagram of the preset Piper triangular diagram, and connect the coordinates of the cation phase diagram and the anion phase diagram of each water sample to form the topological edge of the hydrochemical phase diagram of the metal deposit. Step 2: Determine the initial water source type of the water sample based on the topological similarity between the topological edges of the water chemical phase diagram of various preset standard water sources and the topological edges of the water chemical phase diagram; Step 3: Based on the rate of change of the basic hydrochemical parameters of the water sample over time and the degree of deviation from the standard mineral dissolution equilibrium constant corresponding to the initial water source type, calculate the water-rock interaction activity index to dynamically assess the risk status of the water inflow channel of the metal deposit.

2. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 1, characterized in that, The process of projecting the major ion concentration of each water sample onto the pre-defined Piper triangular diagram of anions and cations is as follows: After normalizing the concentration values ​​of sodium, potassium, calcium, and magnesium ions in each water sample, they are mapped to the coordinates of the inner points of the cation triangle diagram in the preset Piper triangular diagram to generate the cation phase diagram coordinates of each water sample. After normalizing the concentration values ​​of chloride ions, sulfate ions, and bicarbonate ions in each water sample, they are mapped to the corresponding coordinate points of the anion triangular diagram in the Piper triangular diagram to generate the anion phase diagram coordinates of each water sample.

3. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 2, characterized in that, The process of generating the cation phase diagram coordinates for each water sample is as follows: The total cations are the sum of the concentrations of sodium, potassium, calcium, and magnesium ions in the water sample, and the normalized concentration is the ratio of the concentration of each ion to the total cations. Based on the definition of the interior point coordinates of the cation triangle in the Piper triangular diagram, the normalized concentration values ​​are respectively assigned as the weighting coefficients of the interior point coordinates in the directions of the three vertices in the cation triangle. Based on the weighting coefficients, the concentrations of each ion in each water sample are weighted and averaged to obtain the cation phase diagram coordinates of each water sample.

4. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 3, characterized in that, The process of connecting the coordinates of the cation phase diagram and the coordinates of the anion phase diagram generated from each water sample to form the topological edge of the hydrochemical phase diagram of the metal deposit is as follows: Using the central rhomboid region of the Piper tri-line diagram as the connecting plane, and taking the coordinates of the cation phase diagram belonging to the same water sample as the starting point and the coordinates of the anion phase diagram as the ending point, draw straight line segments within the central rhomboid region; The straight line segment is used as the topological edge of the hydrochemical phase diagram of the water sample.

5. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 1, characterized in that, The process of determining the initial water source type of the water sample based on the topological similarity between the topological edges of the hydrochemical phase diagrams of various preset standard water sources and the topological edges of the hydrochemical phase diagrams is as follows: The preset standard water sources include the standard topological edges of roof water sources, structural fissure water sources, and old void water sources. Calculate the Fraser distance between the topological edges of the hydrochemical phase diagram of the water sample and various standard topological edges, and determine the water source type corresponding to the standard topological edge with the smallest Fraser distance as the initial water source type of the water sample.

6. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 5, characterized in that, The process of calculating the Fréchet distances between the topological edges of the hydrochemical phase diagram of the water sample and the preset standard water sources is as follows: Within the central rhomboid region of the Piper trilinear diagram, the topological edges of the hydrochemical phase diagram of the water sample and each of the standard topological edges are discretely sampled with the same preset arc length step size to obtain the first discrete point sequence of the water sample and the second discrete point sequence of each of the standard topological edges. Calculate the Euclidean distance between each discrete point pair between the first discrete point sequence and each of the second discrete point sequences; The minimum value of the supremum among all Euclidean distances is taken as the Fraser distance between the topological edge of the water sample's hydrochemical phase diagram and the preset standard water sources.

7. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 6, characterized in that, The rate of change of the basic hydrochemical parameters of the water sample over time is as follows: According to the equal time sampling period, water samples are continuously taken from each sampling point in the metal deposit, and the water temperature, conductivity, pH, total dissolved solids and content of major and minor ionic components of each group of water samples are measured simultaneously to form the basic hydrochemical parameters of the water samples. Nonlinear trend fitting is performed on the basic hydrochemical parameters of the water sample, and the obtained gradual change rate and fluctuation change rate are combined to form the comprehensive time change rate of the basic hydrochemical parameters.

8. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 7, characterized in that, The degree of deviation from the standard mineral dissolution equilibrium constant corresponding to the initial water source type is used to calculate the water-rock interaction activity index, and the process is as follows: Based on the comprehensive time change rate of each basic hydrochemical parameter, the water-rock reaction process between groundwater and surrounding rock minerals in the metal deposit is inverted to obtain the actual mineral dissolution equilibrium constant of the metal deposit; Based on the standard mineral dissolution equilibrium constant spectrum under the mineral system corresponding to the initial water source type, and the multi-dimensional comparison results between the actual mineral dissolution equilibrium constant, the water-rock interaction activity index of the metal deposit is calculated.

9. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 8, characterized in that, The water-rock interaction activity index of the metal deposit is determined as follows: The multi-dimensional comparison results include the deviation of ion group distribution ratio, the deviation of concentration time decay, and the deviation of acid-base buffering capacity; Based on the stratigraphic lithology, structural fragmentation, and groundwater runoff conditions of the metal deposit, corresponding geological constraint weights are assigned to the three types of characteristic deviations. Based on the geological constraint weights, the water-rock interaction activity index of the metal deposit is calculated, wherein the calculation formula for the water-rock interaction activity index is as follows: ； In the formula, This represents the water-rock interaction activity index. This indicates the deviation of the ion group distribution ratio. This represents the geological constraint weight corresponding to the deviation of the ion group distribution ratio. This indicates the deviation of the concentration from the time-series decay. This represents the geological constraint weight corresponding to the concentration time-series decay deviation. This indicates the deviation of the acid-base buffering capacity. This represents the geological constraint weight corresponding to the deviation of the acid-base buffering capacity. This represents the preset water source topology difference correction coefficient. This represents the Fraser distance between the topological edges of the current water sample's hydrochemical phase diagram and the preset standard water sources. This represents the minimum Fraser distance among all sampling points in the metal deposit. This represents the maximum value of the Fraser distance among all sampling points in the metal deposit.

10. The method for analyzing the hydrological characteristics of a metal deposit as described in claim 9, characterized in that, The process of dynamically assessing the risk status of the water inflow channels in the metal deposit is as follows: Based on historical water inrush cases of the metal deposit, the critical values ​​of the first and second thresholds are graded and calibrated. When the water-rock interaction activity index is between the benchmark value and the first threshold, the water-conducting channel of the metal deposit is determined to be in a stable and normal state. When the water-rock interaction activity index exceeds the first threshold but does not reach the second threshold, it is determined that the water-conducting channel fractures of the metal deposit are expanding and the degree of activation is continuously intensifying. When the water-rock interaction activity index exceeds the second threshold, it is determined that the surrounding rock fissures of the metal deposit are connected and the water-conducting channels are unstable, posing a risk of water inrush in the roadway or working face.

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