A method for determining the groundwater dynamic field of a drought-prone river basin

Abstract

The present invention relates to a method for determining the groundwater dynamic field in a drought-stricken river basin. The method includes: establishing a hydrogeological conceptual model for multiple profiles according to the geological conditions in the study area; generalizing the groundwater in the study area into a two-dimensional steady flow mathematical model of heterogeneous anisotropy based on the hydrogeological conceptual model; determining the flow field distribution map of each profile among the multiple profiles based on the simulation results of the two-dimensional steady flow mathematical model of heterogeneous anisotropy; determining the rate of groundwater runoff based on the flow field distribution map of each profile; establishing a groundwater dynamic field based on the rate of groundwater runoff, so as to be able to determine the relationship between surface water circulation and groundwater transformation, and further provide technical support for the sustainable development and utilization of water resources and the ecological protection and restoration in arid inland basins.

Description

Technical Field

[0001] The present invention relates to the technical field of ecological environment restoration, and particularly to a method for determining the groundwater dynamic field in a drought-stricken river basin. Background Art

[0002] Guided by the regional groundwater system theory, with the research objectives of the conversion relationship of basin water resources, the cyclic evolution of groundwater, and the maintenance of the ecosystem, analyze the changes in glacier reserves, surface runoff characteristics, the evolution law of the groundwater flow field pattern, ecosystem changes, and the characteristics of the basin aquifer structure in the designated research area, and summarize and form technical methods for the sound development of the conversion of basin water resources and the ecosystem, so as to provide technical support for the sustainable development and utilization of water resources and the ecological protection and restoration in arid inland basins.

[0003] Currently, the elements of glaciers, precipitation, surface water, and groundwater in the research area (for example, the arid area in the northwest) are frequently converted, especially the conversion between surface water and groundwater is close. However, the existing research has problems of insufficient quantitative evaluation of the conversion relationship and insufficient quantitative characterization of the hydrodynamic evolution process during the conversion process.

[0004] Therefore, there is an urgent need for a method for determining the groundwater dynamic field in a drought-stricken river basin. Summary of the Invention

[0005] (I) Technical Problems to be Solved

[0006] In view of the above-mentioned disadvantages and deficiencies of the prior art, the present invention provides a method for determining the groundwater dynamic field in a drought-stricken river basin, which solves the technical problems of insufficient quantitative evaluation of the conversion relationship and insufficient quantitative characterization of the hydrodynamic evolution process in the prior art.

[0007] (II) Technical Solutions

[0008] In order to achieve the above object, the main technical solutions adopted by the present invention include:

[0009] In a first aspect, an embodiment of the present invention provides a method for determining the groundwater dynamic field in a drought-stricken river basin, the method comprising: establishing a hydrogeological conceptual model of multiple profiles according to the geological conditions in the research area; generalizing the groundwater in the research area into a non-homogeneous anisotropic two-dimensional steady flow mathematical model according to the hydrogeological conceptual model; determining the flow field distribution map of each profile among the multiple profiles based on the simulation results of the non-homogeneous anisotropic two-dimensional steady flow mathematical model; determining the rate of groundwater runoff based on the flow field distribution map of each profile; and establishing a groundwater dynamic field based on the rate of groundwater runoff.

[0010] In a possible embodiment, the non-homogeneous anisotropic two-dimensional steady flow mathematical model is:

[0011]

[0012] In the formula, K x is the seepage parameter in the horizontal direction x; K z is the seepage parameter in the vertical direction z; K n is the seepage parameter in the normal direction n of the boundary; h is the water level elevation; Q is the source-sink term; τ1 is the constant head boundary; q(x, z) is the unit width flow on the boundary; τ2 is the constant flow boundary; is the head distribution on the boundary.

[0013] In a possible embodiment, K z is measured by a permeameter experiment for measuring the seepage of surface water in a river channel.

[0014] In a possible embodiment, the calculation formula of K z is as follows:

[0015]

[0016] In the formula, L is the thickness of the riverbed sediment inside the inner ring; h 0 is the initial water level of the water supply bucket used in the permeameter experiment; h i is the reading of the second pipe used in the permeameter experiment corresponding to the water level of the water supply bucket and the water level of the outer ring at the same moment t i

[0017] In a possible embodiment, K z is measured by a vertical pipe test for the infiltration of surface water in a river channel.

[0018] In a possible embodiment, the calculation formula of K z is as follows:

[0019] In the formula, h is the water level in the pipe during the experiment; h 0 is the initial water level in the pipe during the test; L is the thickness of the riverbed sediment in the pipe; t 1 is the time.

[0020] In a possible embodiment, the method for determining K x includes: obtaining the first content of tritium element in groundwater, the second content of deuterium element in groundwater, and the third content of oxygen element in groundwater; substituting the first content, the second content, and the third content into the calculation formula of K x to obtain the value of K x ; wherein, the calculation formula of K x is:

[0021] wherein, a represents the slope of the relationship curve; δD represents the second content; δ​18 O represents the third content; T represents the first content; t 2 represents the isotope migration time; b represents a preset formation empirical parameter.

[0022] In a second aspect, an embodiment of the present application provides a storage medium, on which a computer program is stored. When the computer program is run by a processor, the method described in the first aspect or any optional implementation manner of the first aspect is executed.

[0023] In a third aspect, an embodiment of the present application provides an electronic device, including: a processor, a memory, and a bus. The memory stores machine-readable instructions executable by the processor. When the electronic device runs, communication between the processor and the memory is carried out through the bus. When the machine-readable instructions are executed by the processor, the method described in the first aspect or any optional implementation manner of the first aspect is executed.

[0024] In a fourth aspect, the present application provides a computer program product. When the computer program product runs on a computer, the computer is enabled to execute the method in the first aspect or any possible implementation manner of the first aspect.

[0025] (III) Beneficial Effects

[0026] The beneficial effects of the present invention are as follows:

[0027] In the embodiment of the present application, by establishing a hydrogeological conceptual model of multiple profiles according to the geological conditions in the study area, and generalizing the groundwater in the study area into a mathematical model of two-dimensional steady flow of heterogeneous anisotropy according to the hydrogeological conceptual model, and determining the flow field distribution map of each profile in the multiple profiles based on the simulation results of the mathematical model of two-dimensional steady flow of heterogeneous anisotropy, and determining the rate of groundwater runoff based on the flow field distribution map of each profile, and establishing a groundwater dynamic field based on the rate of groundwater runoff, the relationship between surface water circulation and groundwater transformation can be determined, and thus technical support can be provided for the sustainable development and utilization of water resources and the ecological protection and restoration in arid inland basins.

[0028] To make the above objects, features, and advantages to be achieved in the embodiments of the present application more obvious and understandable, the following specific preferred embodiments are given, and in conjunction with the accompanying drawings, the detailed description is as follows. Description of the Drawings

[0029] To more clearly illustrate the technical solutions in the embodiments of the present application, the following briefly introduces the drawings required to be used in the embodiments of the present application. It should be understood that the following drawings only show some embodiments of the present application, and therefore should not be regarded as limiting the scope. For those of ordinary skill in the art, other related drawings can also be obtained based on these drawings without creative efforts.

[0030] Figure 1 Shows a flowchart of a method for determining the groundwater flow field in an arid area basin provided by an embodiment of the present application;

[0031] Figure 2 Shows a schematic diagram of a numerical simulation profile distribution map provided by an embodiment of the present application;

[0032] Figures 3A to 3E Respectively show schematic diagrams of a hydrogeological conceptual model of section one to a hydrogeological conceptual model of section five provided by an embodiment of the present application;

[0033] Figure 4A Shows a schematic diagram of an experimental device used in a piezometer experiment for surface water seepage in a river channel provided by an embodiment of the present application;

[0034] Figure 4B Shows a schematic diagram of a graph of the variation of U - tube readings hA and hB with time provided by an embodiment of the present application;

[0035] Figure 5 Shows a schematic diagram of an experimental device used in a head - drop vertical tube permeability test provided by an embodiment of the present application;

[0036] Figures 6A to 6E Respectively show a flow field distribution map corresponding to section one and flow field distribution maps corresponding to sections two to five provided by an embodiment of the present application;

[0037] Figures 7A to 7E Respectively show schematic diagrams of a groundwater flow velocity distribution map corresponding to section one and groundwater flow velocity distribution maps corresponding to sections two to five provided by an embodiment of the present application. Detailed implementation manner

[0038] For better explaining the present invention for easy understanding, the present invention will be described in detail below with reference to the accompanying drawings through specific implementation manners.

[0039] The solution for determining the groundwater flow field in an arid area basin proposed by the embodiment of the present application, by establishing hydrogeological conceptual models of multiple sections according to the geological conditions in the research area, and generalizing the groundwater in the research area into a non - homogeneous anisotropic two - dimensional steady - flow mathematical model according to the hydrogeological conceptual models, and based on the simulation results of the non - homogeneous anisotropic two - dimensional steady - flow mathematical model, determining the flow field distribution map of each section among multiple sections, and based on the flow field distribution map of each section, determining the rate of groundwater runoff, and based on the rate of groundwater runoff, establishing a groundwater flow field, so as to be able to determine the relationship between surface water circulation and groundwater transformation, and further be able to provide technical support for the sustainable development and utilization of water resources and ecological protection and restoration in arid inland basin areas.

[0040] Moreover, through the characterization of the hydrodynamic process in three-dimensional scale, the study of the permeability coefficient and its water resource conversion amount in the embodiments of the present application, the hydrodynamic evolution process after the surface water is converted into groundwater is determined, providing technical method support for the water resource evaluation at the basin scale in arid areas.

[0041] To better understand the above technical solutions, the exemplary embodiments of the present invention will be described in more detail below with reference to the accompanying drawings. Although the exemplary embodiments of the present invention are shown in the drawings, it should be understood that the present invention can be implemented in various forms and should not be limited by the embodiments set forth herein. On the contrary, these embodiments are provided to enable a more clear and thorough understanding of the present invention and to fully convey the scope of the present invention to those skilled in the art.

[0042] Please refer to Figure 1 , Figure 1 which shows a flowchart of a method for determining the groundwater dynamic field in an arid area basin provided by the embodiments of the present application. As Figure 1 shown, the method can be executed by a device for determining the groundwater dynamic field in an arid area basin, and the specific device of the device can be set according to actual needs, and the embodiments of the present application are not limited thereto. For example, the device can be a computer or a server, etc. Specifically, the method includes:

[0043] Step S110, establish a hydrogeological conceptual model of multiple profiles according to the geological conditions in the study area.

[0044] It should be understood that the specific area of the study area can be set according to actual needs, as long as it is ensured that the study area includes the arid area and the basin passing through the arid area, and the embodiments of the present application are not limited thereto.

[0045] Optionally, the study area can be the Hotan River Basin.

[0046] It should also be understood that the specific process of establishing a hydrogeological conceptual model of multiple profiles according to the geological conditions in the study area can also be set according to actual needs, and the embodiments of the present application are not limited thereto.

[0047] Optionally, affected by various factors such as the spatial structure of the aquifer and the topography and geomorphology in the study area, the groundwater circulation characteristics in the study area are very complex. In order to reveal the groundwater circulation characteristics in the horizontal and vertical directions in the study area, typical profiles can be used for detailed research to reveal the characteristics of groundwater hydrodynamics, groundwater hydrochemistry, groundwater age, etc. during the groundwater flow process, and to characterize the hierarchical structure of the groundwater flow system and the circulation patterns of groundwater at different depths. Moreover, multiple typical profiles can be selected to focus on the study of the distribution characteristics of hydrochemistry and isotopes.

[0048] It should be understood that the specific number of typical profiles can be selected according to actual needs, and the embodiments of the present application are not limited thereto.

[0049] For example, in the case where the study area is the Hotan River Basin, 5 typical profiles (i.e., Profile 1 to Profile 5) can be selected, and the profile positions in the basin are as Figure 2 shown.

[0050] Here, it should be noted that Figures 3A to 3E 、 Figures 6A to 6E and Figures 7A to 7E are the attached drawings corresponding to the 5 typical profiles in Figure 2 .

[0051] In addition, according to the lithology revealed by boreholes, the lithology of the aquifer includes cobble gravel, sandy gravel, sand, and clay. The upstream aquifer has good water permeability, and the downstream has poor permeability. Also, according to the characteristics of the aquifer lithology, the aquifer grid can be divided into multiple layers (e.g., 3 layers) vertically. The aquifer parameter partition is determined according to the hydrogeological profile characteristics and the pumping test results of the boreholes. The horizontal permeability coefficient is determined according to the pumping test results, and the vertical permeability coefficient of the aquifer adopts an empirical value. The ratio of the given horizontal permeability coefficient to the vertical permeability coefficient in the numerical simulation of this profile can be 100 to 1000. The hydrogeological conceptual model diagrams of each profile are as Figures 3A to 3E . Among them, Figure 3E The horizontal and vertical coordinates of Figures 3A to 3D are the same as those of

[0052] Step S120, according to the hydrogeological conceptual model, generalize the groundwater in the study area into a two-dimensional steady flow mathematical model of inhomogeneous anisotropy.

[0053] Specifically, according to the available formation data and balance data, the groundwater movement can be generalized into a two-dimensional steady flow of inhomogeneous anisotropy. According to the hydrogeological conceptual model, the two-dimensional steady flow of inhomogeneous anisotropy can be expressed as:

[0054]

[0055] In the formula, K x is the permeability parameter in the horizontal direction x, and its unit can be m / d; K z is the permeability parameter in the vertical direction z, and its unit can be m / d; K n is the permeability parameter in the normal direction n of the boundary, and its unit can be m / d; h is the water level elevation, and its unit can be m; Q is the source-sink term, and its unit can be 1 / d; τ1 is the constant head boundary; q(x,z) is the unit-width flow on the boundary, and its unit can be m / d; τ2 is the constant flow boundary; is the head distribution on the boundary.

[0056] It should be understood that the acquisition methods of the various parameters in the above homogeneous anisotropic two-dimensional steady flow mathematical model can be set according to actual needs, and the embodiments of the present application are not limited thereto.

[0057] Optionally, K z is measured by a piezometer experiment for measuring the infiltration of river surface water.

[0058] Specifically, the plain oasis in the study area depends on a large amount of diverted surface water for irrigation to survive and develop. With the expansion of artificial oases and the introduction of surface water into oasis irrigation, complex conversions of surface water-evaporation-unsaturated zone water-groundwater moisture occur between the surface and groundwater. The conversion amount is related to irrigation methods, irrigation quotas, crop types, groundwater table depth, unsaturated zone lithological structure, and soil moisture content before irrigation, etc. Therefore, revealing the irrigation water infiltration mechanism and judging the irrigation water recharge intensity under different conditions are the key points for the conversion of surface water and groundwater in the oasis plain area. The research of this application intends to reveal the irrigation water infiltration characteristics under the local irrigation mode through in-situ experiments in the oasis plain area, calculate the infiltration coefficient, and provide basic parameters for the calculation of surface water and groundwater conversion.

[0059] Please refer to Figure 4, Figure 4A which shows a schematic diagram of an experimental device used in a piezometer experiment for the infiltration of river surface water provided by an embodiment of the present application. Among them, hA can represent the reading of tube A in the U-shaped tube, and hB can represent the reading of tube B in the U-shaped tube.

[0060] And, Figure 4B which shows a schematic diagram of a graph of the changes of the U-shaped tube readings hA and hB with time provided by an embodiment of the present application. Thus, on the basis of Figure 4A and Figure 4B , the vertical infiltration parameter K at different river water depths can be calculated through the curve slope z .

[0061] During the experiment, the ground is used as the zero reference plane, and the water level in the water supply bucket in the experimental device is h. Then, according to Darcy's law, the calculation formula for the vertical infiltration parameter can be obtained:

[0062]

[0063] In the formula, L is the thickness of the riverbed sediment inside the inner ring, and its unit is cm; h 0 is the initial water level of the water supply bucket used in the piezometer experiment, and its unit is cm; h i is the reading of the second tube used in the piezometer experiment corresponding to the water level of the water supply bucket and the water level of the outer ring at the same moment t i , and its unit is cm.

[0064] Optionally, Kz It is measured through the vertical pipe test of river channel surface water infiltration.

[0065] Specifically, the vertical pipe test of river channel surface water infiltration is applicable to measuring the infiltration parameters in the vertical direction. This method can be used in the fine soil zone to study the variability of riverbed sediments at different depths and the variability of infiltration parameters perpendicular to the vertical direction. The head-drop vertical pipe infiltration test is as Figure 5 shown, and its working principle is Darcy's law. Among them, in this test, a PVC pipe with a length of 120 cm and a pipe diameter of 50 mm can be used as the test equipment. Of course, it should be understood that the relevant parameters of the test equipment can also be set according to actual needs, and the embodiments of the present application are not limited thereto.

[0066] And, the calculation formula of K z is as follows:

[0067]

[0068] In the formula, h is the water level in the pipe during the experiment; h 0 is the initial water level in the pipe during the test; L is the thickness of the riverbed sediment in the pipe; t 1 is the time.

[0069] Optionally, the determination method of K x is as follows: Obtain the first content of tritium element in groundwater, the second content of deuterium element in groundwater, and the third content of oxygen element in groundwater; Substitute the first content, the second content, and the third content into the calculation formula of K x to obtain the value of K x ; Among them, the calculation formula of K x is:

[0070] Among them, a represents the slope of the relationship curve; δD represents the second content; δ 18 O represents the third content; T represents the first content; t 2 represents the isotope migration time; b represents the preset formation empirical parameter.

[0071] It should also be understood that a, t 2 and b can also be referred to as the specified first parameter, the specified second parameter, and the specified third parameter, etc.

[0072] It should be noted here that each point in space has a K x value.

[0073] In addition, the hydraulic gradient I can also be calculated according to the measured flow field, the area S can be determined according to the infiltration cross-section, and the recharge amount Q 补 is calculated. Specifically, the calculation formula of the recharge amount Q 补 is as follows:

[0074]

[0075] wherein, t 3 is the time.

[0076] Step S130: Based on the simulation results of the heterogeneous anisotropic two-dimensional steady flow mathematical model, determine the flow field distribution map of each profile among multiple profiles.

[0077] It should be noted here that existing methods can be used to process the simulation results of the heterogeneous anisotropic two-dimensional steady flow mathematical model to obtain the flow field distribution map of each profile among multiple profiles.

[0078] In addition, Figures 6A to 6E the flow field distribution maps corresponding to Profile 1 to Profile 5 are respectively shown. And Figures 6A to 6E the abscissa of

[0079] Step S140: Based on the flow field distribution map of each profile, determine the rate of groundwater runoff.

[0080] It should be noted here that existing methods can be used to process the flow field distribution map of each profile to obtain the permeability parameter and the hydraulic gradient, and based on the permeability parameter and the hydraulic gradient, calculate the rate of groundwater runoff.

[0081] It should be understood that the calculation process of the rate of groundwater runoff can be set according to actual needs, and the embodiments of the present application are not limited thereto.

[0082] For example, the rate of groundwater runoff can be calculated by the following formula:

[0083] V = KI;

[0084] wherein, V can represent the rate of groundwater runoff; K can represent the permeability parameter; I can represent the hydraulic gradient.

[0085] It should be noted here that the value of I is the quotient of the elevation difference of the groundwater level between two points and the vertical distance therebetween; the value of K is determined by actual measurement of the pumping test of the borehole.

[0086] And, based on Darcy's law, the groundwater flow velocity distribution map as shown in Figures 7A to 7E can be obtained according to the flow field of each profile, and the abscissa of the groundwater flow velocity distribution map as shown in Figures 7A to 7E can be distance, and the ordinate can be elevation.

[0087] Step S150: Based on the rate of groundwater runoff, measure the elevation of the groundwater level and establish a groundwater dynamic field.

[0088] Specifically, according to the cross-sectional flow velocity distribution, the groundwater runoff rate is 0.04 - 1.6 m / d. The groundwater dynamic field reveals the groundwater circulation and the relationship between surface water and groundwater transformation.

[0089] Therefore, in the embodiment of the present application, by establishing hydrogeological conceptual models of multiple profiles according to the geological conditions in the study area, generalizing the groundwater in the study area into a heterogeneous anisotropic two-dimensional steady flow mathematical model according to the hydrogeological conceptual models, determining the flow field distribution map of each profile among the multiple profiles based on the simulation results of the heterogeneous anisotropic two-dimensional steady flow mathematical model, determining the rate of groundwater runoff based on the flow field distribution map of each profile, and establishing a groundwater dynamic field based on the rate of groundwater runoff, the relationship between surface water circulation and groundwater transformation can be determined, and thus technical support can be provided for the sustainable development and utilization of water resources and the ecological protection and restoration in arid inland basins.

[0090] In addition, in the embodiment of the present application, through the characterization of the hydrodynamic process at the three-dimensional scale, the study of the permeability coefficient and its water resource conversion amount, the hydrodynamic evolution process after surface water is converted into groundwater is determined, providing technical method support for water resource evaluation at the basin scale in arid areas.

[0091] It should be understood that the above method for determining the groundwater dynamic field in the arid area basin is only exemplary, and those skilled in the art can make various deformations according to the above method, and the deformed solutions also fall within the protection scope of the present application.

[0092] The present application provides a storage medium on which a computer program is stored, and when the computer program is run by a processor, it executes the method described in the embodiment.

[0093] The present application also provides a computer program product, which, when running on a computer, causes the computer to execute the method described in the method embodiment.

[0094] Those skilled in the art should understand that the embodiments of the present invention can be provided as a method, a system, or a computer program product. Therefore, the present invention can adopt the form of a complete hardware embodiment, a complete software embodiment, or an embodiment combining software and hardware aspects. Moreover, the present invention can adopt the form of a computer program product implemented on one or more computer-usable storage media (including but not limited to disk memories, CD-ROMs, optical memories, etc.) containing computer-usable program codes.

[0095] The present invention is described with reference to the flowcharts and / or block diagrams of methods, apparatuses (systems), and computer program products according to embodiments of the present invention. It should be understood that each process and / or block in the flowcharts and / or block diagrams, and the combination of processes and / or blocks in the flowcharts and / or block diagrams, can be implemented by computer program instructions.

[0096] It should be noted that in the claims, any reference signs placed between parentheses shall not be construed as limiting the claim. The word "comprising" does not exclude the presence of elements or steps not listed in a claim. The word "a" or "an" preceding an element does not exclude the presence of a plurality of such elements. The present invention can be implemented by means of hardware including several different elements and by means of a suitably programmed computer. In a claim listing several means, several of these means can be embodied by the same hardware. The use of the terms first, second, third, etc. is for convenience of expression only and does not denote any order. These terms can be understood as part of the name of the element.

[0097] In addition, it should be noted that in the description of this specification, the descriptions of terms such as "one embodiment", "some embodiments", "embodiment", "example", "specific example" or "some examples", etc. refer to the specific features, structures, materials or characteristics described in connection with the embodiment or example being included in at least one embodiment or example of the present invention. In this specification, the schematic descriptions of the above terms do not necessarily refer to the same embodiment or example. Moreover, the specific features, structures, materials or characteristics described can be combined in a suitable manner in any one or more embodiments or examples. In addition, without contradiction, those skilled in the art can combine and combine the different embodiments or examples described in this specification and the features of different embodiments or examples.

[0098] Although the preferred embodiments of the present invention have been described, those skilled in the art can make additional changes and modifications after learning the basic creative concept. Therefore, the claims should be construed to include the preferred embodiments as well as all changes and modifications falling within the scope of the present invention.

[0099] Obviously, those skilled in the art can make various modifications and variations to the present invention without departing from the spirit and scope of the present invention. Thus, if these modifications and variations of the present invention fall within the scope of the claims of the present invention and their equivalent technologies, the present invention should also include these modifications and variations.

Claims

1. A method for determining the groundwater dynamic field in a drought-prone river basin, characterized in that, comprising: establishing a hydrogeological conceptual model for multiple profiles according to the geological conditions in the study area; generalizing the groundwater in the study area into a heterogeneous anisotropic two-dimensional steady flow mathematical model according to the hydrogeological conceptual model; determining the flow field distribution map of each profile among the multiple profiles based on the simulation results of the heterogeneous anisotropic two-dimensional steady flow mathematical model; determining the rate of groundwater runoff based on the flow field distribution map of each profile; establishing the groundwater dynamic field based on the rate of groundwater runoff; the heterogeneous anisotropic two-dimensional steady flow mathematical model is: Where, K x is the seepage parameter in the horizontal direction x; K z is the seepage parameter in the vertical direction z; K n is the seepage parameter in the boundary normal direction n; h(x, z) is the water level elevation on the boundary; Q is the source-sink term; τ1 is the constant head boundary; q(x, z) is the unit width flow rate on the boundary; τ2 is the constant flow boundary; is the head distribution on the boundary.

2. The method according to claim 1, characterized in that, The described K z is measured by the infiltrometer experiment for measuring the infiltration of surface water in the river channel.

3. The method according to claim 2, characterized in that, The said K z has the following calculation formula: where L is the thickness of the riverbed sediment inside the inner ring; h 0 is the initial water level of the water supply bucket used in the permeameter experiment; h i is the reading of the second pipe used in the permeameter experiment corresponding to the water levels of the water supply bucket and the outer ring at the same time t i ​ 4. The method according to claim 1, characterized in that, The K z is measured through the vertical pipe test of river surface water infiltration.

5. The method according to claim 4, characterized in that, The said K z has the following calculation formula: where h is the water level in the pipe during the experiment; h 0 is the initial water level in the pipe during the test; L is the thickness of the riverbed sediment in the pipe; t 1 is time.

6. The method according to claim 1, characterized in that, The described K x The determination method includes: obtaining a first content of tritium element in groundwater, a second content of deuterium element in groundwater, and a third content of oxygen element in groundwater; Substitute the first content, the second content, and the third content into the calculation formula of K x to obtain the value of K x ; wherein, the calculation formula of K x is: where a represents the slope of the relationship curve; δD represents the second content; δ 18 O represents the third content; T represents the first content; t 2 represents the isotope migration time; b represents a preset formation empirical parameter.

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