CN117172142B - Hydrological model water flow along-path distribution considering terrain influence - Google Patents
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Abstract
The hydrological model water flow path-along distribution taking the influence of the terrain into consideration comprises the following steps: 1. dispersing a river basin into a plurality of grid units, setting the resolution of the grid units as a calculation scale for the confluence calculation of the distributed hydrological model, and extracting the terrain gradient beta c; 2. the resolution of the grid unit is improved, the terrain gradient is calculated, the terrain gradient is upscaled to the calculated scale, and the terrain fluctuation beta s in the grid unit is quantized; 3. taking rainfall P and evaporation E as inputs, calculating water flow q which can flow out freely in the grid unit, and dividing q into water flow q c entering a downstream grid unit air-packing belt and water flow q s discharged into an internal channel of the grid unit; 4. the water flow q c is supplemented with the water shortage amount of the air-packing belt of the downstream grid unit and then continuously flows out, and the water flow q s rapidly moves among different grid units through the channels, so that the water flow along-path redistribution among the grid units is realized. The method has reasonable design, is favorable for better simulating the space-time dynamic distribution of soil water in the rainfall runoff process, and realizes the runoff process simulation with higher precision.
Description
Technical Field
The invention relates to the technical field of hydrology, in particular to a hydrological model water flow along-path distribution method considering the influence of terrain.
Background
Watershed water circulation can be generalized to the processes of precipitation, evapotranspiration, runoff, and watershed water storage capacity change, wherein precipitation is the main input of the circulation process and usually plays a dominant role; the water loss caused by the evaporation is an output item of the water circulation process; the dynamic change of runoff and water storage capacity of a river basin is jointly influenced by precipitation and evapotranspiration, and is a key link influencing natural ecological environment and human society in water circulation of the river basin. The space-time dynamic distribution of the water content of the soil directly influences the evolution of the soil ecosystem, and forms important basis for dividing the Chinese climate and vegetation types together with factors such as rainfall, thereby influencing the crop types and cultivation modes in different regions and indirectly modeling the economic, cultural and social life modes with various characteristics. Therefore, the dynamic change of the water content of the soil is used as a key link of water circulation of the river basin, the influence of meteorological factors and topographical features on the space-time distribution of the water content of the soil is quantized, the method is beneficial to improving the rationality of the rainfall runoff process simulation of the river basin, and important reference bases are provided for the aspects of soil moisture content simulation and forecast, agricultural production practice, ecological environment protection, human society scientific research and the like.
However, the conventional lumped hydrologic model generally takes a river basin as a whole, and it is difficult to realize quantitative simulation of soil water space-time distribution dynamic process inside the river basin. Based on the development of remote sensing, geographic information, digital watershed and other technologies, the grid digital elevation model (DEM, digital Elevation Model) adopting the numerical matrix to describe the elevation change of the ground surface is gradually mature and is widely applied. Based on a digital elevation model, a distributed hydrological model generally divides a river basin into a plurality of calculation units, water flows are moved and collected among different calculation units, and factors such as terrain gradient and the like are combined, so that water flow along-path redistribution is reasonably considered, and the problems of important points and difficulty in guaranteeing hydrological process simulation precision of the distributed model and improving the soil water space-time dynamic distribution simulation refinement level are solved.
In order to further promote the development of the soil water space-time dynamic distribution simulation and improve the simulation precision of the distributed rainfall runoff process, the influence of the terrain gradient on the water flow path distribution needs to be understood more deeply, and the response of the soil water content of each grid unit to the water flow path movement is quantized.
When researching a distributed hydrological model water flow path-along distribution method, the first challenge is to reasonably divide water flow directly entering a channel and water flow for supplementing the soil water content of a downstream grid unit. In the current practical application, the influence of the terrain gradient on the water flow along-path distribution is not considered, and all water flows are directly supplemented and supplemented with the soil water content of the downstream grid unit. Although the method realizes generalized simulation of water flow exchange among grid units to a certain extent, the space-time dynamic distribution process of soil water in the river basin is difficult to reasonably describe, the simulation precision of the distributed rainfall runoff process is reduced to a certain extent, and the simulation refinement level of the rainfall runoff process is restricted.
Therefore, the method for neglecting the influence of the terrain gradient on the water flow along-path redistribution is not beneficial to the improvement of the simulation refinement level of the soil water space-time dynamic distribution. Therefore, it is necessary to design a water flow path-along-distance distribution method of a hydrological model in consideration of the influence of terrain, so as to overcome the above problems.
Disclosure of Invention
In order to avoid the problems, the hydrologic model water flow along-path redistribution method considering the influence of the terrain is provided, the design is reasonable, the soil water space-time dynamic distribution in the rainfall runoff process is well simulated, and the runoff process simulation with higher precision is realized.
The invention provides a hydrological model water flow along-path distribution method considering the influence of terrain, which comprises the following steps:
Step 1, dispersing a river basin into a plurality of grid units based on a digital elevation model D c, setting the resolution of the grid units as a calculation scale for confluence calculation of a distributed hydrological model, and extracting a terrain gradient beta c;
Step 2, selecting a digital elevation model D s with resolution higher than D c, calculating the terrain gradient, upscaling the terrain gradient to a calculated scale, and quantifying terrain fluctuation beta s in the grid unit;
Step 3, calculating water flow q which can flow out freely in the grid unit by taking rainfall P and evaporation E as inputs, and dividing q into water flow q c entering a downstream grid unit air-packing belt and water flow q s discharged into an internal channel of the grid unit according to the proportion between beta c and beta s;
And 4, supplementing water flow q c with water shortage of the air-packing belt of the downstream grid unit, and continuing to flow out, wherein water flow q s rapidly moves among different grid units through channels, so that water flow along-path redistribution among the grid units is realized.
Preferably, the step 1 comprises the following sub-steps:
1.1, discretizing a drainage basin into a plurality of orthogonal grid units based on a digital elevation model D c, and taking the side length of the grid units as L c as a calculation scale;
1.2 coding 8 adjacent cells of the grid cells in a clockwise direction, coding adjacent grid cells in the east, southeast, south, southwest, west, northwest, north and northeast directions as 0,1, 2, 3,4, 5,6 and 7, respectively;
1.3, taking the direction of the grid unit with the lowest relative elevation as the flow direction of water flow, taking the grid unit into which the water flow flows as the downstream grid unit, and calculating the terrain gradient beta c between the grid unit and the downstream grid unit, wherein the calculation formula is as follows:
Wherein: e c is the grid cell elevation; e x is the downstream grid cell elevation; a straight line distance between the grid unit and the downstream grid unit; when the downstream grid cell codes 0, 2,4, and 6, the value of ε is 1, otherwise it is 1.414.
Preferably, the step 2 includes the following sub-steps:
2.1, selecting a digital elevation model D s with resolution higher than D c, and dispersing grid units into a plurality of small grid units with side length L s;
2.2 calculating the terrain gradient beta s between the small grid units with the side length of L s in the grid units by adopting the methods in the steps 1.2 and 1.3;
2.3 calculating a first order origin moment of the terrain gradient beta s, upscaling to a calculation scale, quantifying the terrain fluctuation beta σ inside the grid unit, and the calculation formula is as follows:
Wherein: i is the number of a small grid unit with the side length L s inside the grid unit, and the number is from 1 to n; n is the number of small grid cells with side length L s inside the grid cells.
Preferably, the step3 includes the following sub-steps:
3.1, using rainfall P and evaporation E as input, and calculating water flow q which can flow out freely in the grid unit by adopting a full-reservoir flow model and a linear reservoir formula;
3.2 dividing the water flow q into a water flow q c entering the downstream grid unit air-packing belt and a water flow q s discharged into the grid unit internal channel according to the ratio between beta c and beta s, and calculating the following formula:
qc+qs＝q；
Preferably, the step 4 includes the following sub-steps:
4.1 the water flow q c is continuously flowed out after supplementing the air-packing belt water-shortage quantity of the downstream grid unit,
When w+pe+q c is less than or equal to WM, r=0;
When w+pe+q c > WM, r=pe+w+q c -WM;
wherein: WM is the water storage capacity of the tension water; w is tension water content; PE is rainfall after evaporation loss is deducted, namely net rain; r is the generated runoff amount;
the runoff amount R is converted into a water flow q b capable of flowing after being calculated by a water diversion source of a full-reservoir flow model and a linear reservoir method;
4.2, fast moving the water flow Q s between different grid units through the channels, solving the water flow Q through the following two formulas simultaneously to obtain the channel water flow Q, and then gradually accumulating to obtain the runoff process of the outlet of the river basin;
Wherein: a is the cross-sectional area of channel water flow, Q is the channel water flow; s f is the hydraulic gradient, and S o is the channel gradient; t is a time term, and the value is generally a calculation time interval; x is a spatial term and the value is typically the side length of the grid cell.
Compared with the prior art, the invention has the following beneficial effects: the water flow path redistribution of the hydrological model considering the terrain influence is based on physical factors influencing the water flow path redistribution, so that the influence of the terrain on the water flow path redistribution is quantified, and a distributed hydrological model water flow path redistribution method considering the terrain influence is further provided; the accuracy and the reliability of the calculation result are guaranteed, and meanwhile the problem of along-path redistribution when water flows in the distributed model pass through different calculation grid units is solved. The method mainly uses a basin digital elevation model, has stable and reliable data sources, has definite functional relation among variables in the method, is beneficial to the rapid and automatic execution of the water flow along the course in the basin, simplifies the extraction step by a digital basin technology, ensures the objective rationality of the result, and can further promote the deep development of digital hydrology and a distributed model.
Drawings
FIG. 1 is a flow chart of a hydrological model water flow along-path redistribution method taking into account terrain effects according to a preferred embodiment of the present invention;
FIG. 2 is a digital elevation model of a basin;
FIG. 3 is a flow direction encoding schematic;
FIG. 4 is a gradient calculation illustration;
FIG. 5 shows the slope of a basin before upscaling;
FIG. 6 shows the slope of a river basin after upscaling;
FIG. 7 is a water flow division schematic;
FIG. 8 is a 20200915 th soil water spatial distribution for flood process 8 h;
FIG. 9 is a water space distribution of soil at 9h during 20200915 th flood;
FIG. 10 is a water-in-soil spatial distribution at 10h during the 20200915 th flood;
FIG. 11 is a 20200915 th spatial distribution of soil water at 11h during flood;
FIG. 12 is a water space distribution of soil at 12h in 20200915 th flood process;
FIG. 13 is a soil water spatial distribution at 13h in the 20200915 th flood process;
FIG. 14 is a soil water spatial distribution at 14h during 20200915 th flood;
FIG. 15 is a 15h soil water spatial distribution for 20200915 th flood process;
FIG. 16 is a soil water spatial distribution at 16h for the 20200915 th flood process;
FIG. 17 is a 20200915 flood process simulation result;
FIG. 18 is a comparison of the results of a simulation of LPRM AMSR2 product in a river basin with soil water;
FIG. 19 shows the proportion of soil moisture content in the total amount of the river basin in different areas.
Detailed Description
As shown in fig. 1 to 19, the water flow path-along distribution method of the hydrological model taking the influence of terrain into consideration provided by the embodiment includes the following steps:
Step 1, dispersing a river basin into a plurality of grid units based on a digital elevation model D c, setting the resolution of the grid units as a calculation scale for confluence calculation of a distributed hydrological model, and extracting a terrain gradient beta c;
The method comprises the following substeps:
1.1, discretizing a drainage basin into a plurality of orthogonal grid units based on a digital elevation model D c, and taking the side length of the grid units as L c as a calculation scale;
1.2 coding 8 adjacent cells of the grid cells in a clockwise direction, coding adjacent grid cells in the east, southeast, south, southwest, west, northwest, north and northeast directions as 0,1, 2, 3,4, 5,6 and 7, respectively;
1.3, taking the direction of the grid unit with the lowest relative elevation as the flow direction of water flow, taking the grid unit into which the water flow flows as the downstream grid unit, and calculating the terrain gradient beta c between the grid unit and the downstream grid unit, wherein the calculation formula is as follows:
Wherein: e c is the grid cell elevation; e x is the downstream grid cell elevation; a straight line distance between the grid unit and the downstream grid unit; when the downstream grid cell codes 0, 2,4, and 6, the value of ε is 1, otherwise it is 1.414.
Step 2, selecting a digital elevation model D s with resolution higher than D c, calculating the terrain gradient, upscaling the terrain gradient to a calculated scale, and quantifying terrain fluctuation beta s in the grid unit;
The method comprises the following substeps:
2.1, selecting a digital elevation model D s with resolution higher than D c, and dispersing grid units into a plurality of small grid units with side length L s;
2.2 calculating the terrain gradient beta s between the small grid units with the side length of L s in the grid units by adopting the methods in the steps 1.2 and 1.3;
2.3 calculating a first order origin moment of the terrain gradient beta s, upscaling to a calculation scale, quantifying the terrain fluctuation beta σ inside the grid unit, and the calculation formula is as follows:
Wherein: i is the number of a small grid unit with the side length L s inside the grid unit, and the number is from 1 to n; n is the number of small grid cells with side length L s inside the grid cells.
Step 3, calculating water flow q which can flow out freely in the grid unit by taking rainfall P and evaporation E as inputs, and dividing q into water flow q c entering a downstream grid unit air-packing belt and water flow q s discharged into an internal channel of the grid unit according to the proportion between beta c and beta s;
The method comprises the following substeps:
3.1, using rainfall P and evaporation E as input, and calculating water flow q which can flow out freely in the grid unit by adopting a full-reservoir flow model and a linear reservoir formula;
3.2 dividing the water flow q into a water flow q c entering the downstream grid unit air-packing belt and a water flow q s discharged into the grid unit internal channel according to the ratio between beta c and beta s, and calculating the following formula:
qc+qs＝q；
Step 4, water flow q c is supplemented with the water shortage amount of the air-packing belt of the downstream grid unit and then continuously flows out, and water flow q s rapidly moves among different grid units through channels, so that water flow along-path redistribution among the grid units is realized;
The method comprises the following substeps:
4.1 the water flow q c is continuously flowed out after supplementing the air-packing belt water-shortage quantity of the downstream grid unit,
When w+pe+q c is less than or equal to WM, r=0;
When w+pe+q c > WM, r=pe+w+q c -WM;
wherein: WM is the water storage capacity of the tension water; w is tension water content; PE is rainfall after evaporation loss is deducted, namely net rain; r is the generated runoff amount;
The runoff amount R is converted into water flow q b capable of continuously flowing after being calculated by a water diversion source of a full-reservoir flow model and a linear reservoir method;
4.2, fast moving the water flow Q s between different grid units through the channels, solving the water flow Q through the following two formulas simultaneously to obtain the channel water flow Q, and then gradually accumulating to obtain the runoff process of the outlet of the river basin;
Wherein: a is the cross-sectional area of channel water flow, Q is the channel water flow; s f is the hydraulic gradient, and S o is the channel gradient; t is a time term, and the value is generally a calculation time interval; x is a spatial term and the value is typically the side length of the grid cell.
Taking a certain river basin in Hunan province as an example, the area of the river basin is 7864km 2, the elevation is 42-1396 m, the flow of the incoming water in the interval is short, the confluence is quick, the burst performance is strong, the influence on the warehouse-in runoff is large, the average rainfall over many years is about 1724mm, and the flood season is mainly concentrated in 4-9 months. There are 23 rainfall stations in the flow area, and the daily rainfall data in 2014-2020 and the period rainfall data of the scene flood are collected.
Taking 20200915 flood process as an example, after the upstream inflow through river channel calculation is added to interval inflow, simulating to obtain a warehouse-in runoff process, applying a distributed hydrological model water flow along-path redistribution method considering the influence of terrain, and outputting the soil water content of 20200915 flood process 8-16 h after rainfall begins.
The hydrological model water flow path-along redistribution method taking the influence of terrain into consideration comprises the following steps:
Step 1, dispersing a river basin into a plurality of orthogonal grid units based on a digital elevation model D c, setting the resolution of the grid units as a calculation scale of confluence calculation of a distributed hydrological model, and extracting a terrain gradient beta c, wherein the method specifically comprises the following steps of:
1.1, discretizing a drainage basin into a plurality of orthogonal grid units based on a digital elevation model D c, and taking the side length of the grid units as L c as a calculation scale, as shown in FIG. 2;
1.2 coding 8 adjacent cells of the grid cells in a clockwise direction, coding adjacent grid cells in the east, southeast, south, southwest, northwest, north and northeast directions as 0, 1, 2, 3, 4, 5, 6 and 7, respectively, as shown in fig. 3;
1.3, taking the direction of the grid unit with the lowest relative elevation as the flow direction of water flow, taking the grid unit into which the water flow flows as the downstream grid unit, calculating the terrain gradient beta c between the grid unit and the downstream grid unit, as shown in fig. 4, and obtaining gradient space distribution in the flow domain, as shown in fig. 5, wherein the calculation formula is as follows:
Wherein: e c is the grid cell elevation, E x is the downstream grid cell elevation, For the straight line distance between the grid cell and the downstream grid cell, the value of e is 1 when the downstream grid cell is coded as 0, 2, 4 and 6, otherwise 1.414.
Step 2, selecting a digital elevation model D s with resolution higher than D c, calculating the terrain gradient and upscaling the terrain gradient to the calculated scale, and quantifying the terrain fluctuation beta σ in the grid unit, wherein the method specifically comprises the following steps of:
2.1, selecting a digital elevation model D s with resolution higher than D c, and further dispersing the grid units into a plurality of small grid units with side length L s;
2.2 calculating the terrain gradient beta s between the small grid units with the side length of L s in the grid units by adopting the methods in the steps 1.2 and 1.3;
2.3 calculating the first order origin moment of the terrain gradient β s, upscaled to calculated scale, quantifying the terrain relief β σ inside the grid unit, as in fig. 6, the calculation formula is as follows:
Wherein: i is the number of a small grid unit with the side length L s inside the grid unit, and the number is from 1 to n; n is the number of small grid cells with side length L s inside the grid cells.
Step 3, taking rainfall P and evaporation E as inputs, calculating water flow q which can flow out freely in a grid unit, dividing q into water flow q c entering a downstream grid unit air-packing belt and water flow q s discharged into a grid unit internal channel according to the proportion between beta c and beta s, and specifically comprising the following steps:
3.1, taking rainfall P and evaporation E as input, and calculating water flow q which can flow out freely in a grid unit by adopting a full-reservoir flow model and a linear reservoir formula;
3.2 dividing the water flow q into a water flow q c entering the downstream grid cell air-packing belt and a water flow q s discharged into the grid cell internal channel in the ratio between beta c and beta s, as shown in fig. 7, the calculation formula is as follows:
qc+qs＝q
And 4, supplementing water flow q c with water shortage of the air-packing belt of the downstream grid unit, and then continuously flowing out, wherein water flow q s rapidly moves among different grid units through channels to realize water flow along-path redistribution among the grid units, and specifically comprises the following steps:
4.1, supplementing water flow q c to the downstream grid unit, and continuing to flow out after the air-packing belt lacks water;
When w+pe+q c is less than or equal to WM, r=0;
When w+pe+q c > WM, r=pe+w+q c -WM;
wherein: WM represents the water storage capacity of the tension water; w represents the tension water content; PE represents the rainfall after deducting the evaporation loss, namely the net rain; r represents the generated runoff amount; the runoff quantity R is converted into water flow q b capable of continuously flowing after being calculated by a water diversion source of a full-reservoir flow model and a linear reservoir method.
4.2, Fast moving the water flow Q s between different grid units through the channel, solving the water flow Q through the following two formulas simultaneously to obtain the channel water flow Q, and then gradually accumulating and calculating each grid unit to obtain the runoff process of the outlet of the river basin;
Wherein: a is the cross-sectional area of channel water flow, Q is the channel water flow; s f is the hydraulic gradient, and S o is the channel gradient; t is a time term, and the value is generally a calculation time interval; x is a spatial term and the value is typically the side length of the grid cell.
Considering the motion process of the water flow q c and the water flow q s comprehensively, the soil water space-time dynamic change is obtained through simulation, as shown in fig. 8to 16.
In order to further verify the rationality of the spatial distribution of the simulated soil water content, the comparison analysis of the simulation result and the satellite remote sensing inversion soil aquatic product LPRM AMSR2 is carried out in the river basin. The LPRM AMSR2 soil and water products are obtained, and the specific time period above the satellite fly-over research river basin in each flood process is checked by combining the disclosed satellite track records, the soil and water spatial distribution obtained by remote sensing inversion in the corresponding time period is shown in fig. 18a, and the obtained soil and water content spatial distribution is simulated as shown in fig. 18b.
It is worth noting that, because the satellite-mounted AMSR2 sensor mainly carries out remote sensing observation on the water content of the soil layer with the depth of 5cm below the surface, and certain difference exists between the water content of the soil layer and the water content of the model simulation, the example does not pay attention to the difference of the water content values of the soil in a specific place, but divides the river basin into a plurality of areas according to satellite observation results, and analyzes the relative size rules of the water content of the soil in different areas in the river basin and the correlation between the LPRM AMSR2 product and the model simulation results. 52 areas are obtained by dividing in the watershed with larger area, and the proportion of the soil water content in different areas to the total amount of the full watershed is calculated respectively, as shown in figure 19. It can be seen that the simulated soil water in the areas numbered 1 to 5, 43 to 45 and 51 is less than the total amount of the full-basin by about 5.1%, 8% and 3.9%, respectively, compared with the LPRM AMSR2 soil water product. By combining drainage basin topography distribution characteristics and rainfall site observation data, the areas are located at boundaries of drainage basins and have larger gradients, so that rapid movement of water flow is facilitated, rainfall is less in the period, and therefore the water content of the soil obtained through simulation is lower. The proportion of the soil water in most areas to the total amount of the full-drainage basin is relatively close, the rank correlation coefficient of the soil water content simulation value and the LPRM AMSR2 product which are changed among different areas is calculated to be 0.47 and higher than the rank correlation coefficient test critical value under the conditions that the sample number is 52 and the significance level is 0.05, and the spatial distribution characteristics of the soil water content simulated by the model can be considered to have positive correlation relation with satellite remote sensing observation results.
Meanwhile, the rainfall runoff process of the river basin obtained based on the simulation of the soil and aquatic products is output and compared with the actual measurement process, as shown in fig. 17. The certainty factor between the simulated rainfall runoff process and the actual measurement process obtained through statistics reaches 0.87, and the error is small.
The comparison analysis of the comprehensive soil water simulation result and the satellite remote sensing inversion soil aquatic product LPRM AMSR2, and the comparison of the basin rainfall runoff process and the actual measurement process can be considered to be reasonable in design, and the distributed hydrologic model water flow along-path redistribution method considering the terrain influence is favorable for better simulating the soil water space-time dynamic distribution in the rainfall runoff process, so that the runoff process simulation with higher precision is realized.
Finally, it should be noted that: the above embodiments are only for illustrating the technical solution of the present invention, and not for limiting the same; although the invention has been described in detail with reference to the foregoing embodiments, it will be understood by those of ordinary skill in the art that: the technical scheme described in the foregoing embodiments can be modified or some or all of the technical features thereof can be replaced by equivalents; such modifications and substitutions do not depart from the spirit of the invention.
Claims (2)
1. The hydrological model water flow path-along-distance redistribution method considering the terrain influence is characterized by comprising the following steps of:
Step 1, dispersing a river basin into a plurality of grid units based on a digital elevation model D c, setting the resolution of the grid units as a calculation scale for confluence calculation of a distributed hydrological model, and extracting a terrain gradient beta c;
Step 2, selecting a digital elevation model D s with resolution higher than D c, calculating the terrain gradient, upscaling the terrain gradient to a calculated scale, and quantifying terrain fluctuation beta s in the grid unit;
Step 3, calculating water flow q which can flow out freely in the grid unit by taking rainfall P and evaporation E as inputs, and dividing q into water flow q c entering a downstream grid unit air-packing belt and water flow q s discharged into an internal channel of the grid unit according to the proportion between beta c and beta s;
Step 4, water flow q c is supplemented with the water shortage amount of the air-packing belt of the downstream grid unit and then continuously flows out, and water flow q s rapidly moves among different grid units through channels, so that water flow along-path redistribution among the grid units is realized;
The step 1 comprises the following substeps:
1.1, discretizing a drainage basin into a plurality of orthogonal grid units based on a digital elevation model D c, and taking the side length of the grid units as L c as a calculation scale;
1.2 coding 8 adjacent cells of the grid cells in a clockwise direction, coding adjacent grid cells in the east, southeast, south, southwest, west, northwest, north and northeast directions as 0,1, 2, 3,4, 5,6 and 7, respectively;
1.3, taking the direction of the grid unit with the lowest relative elevation as the flow direction of water flow, taking the grid unit into which the water flow flows as the downstream grid unit, and calculating the terrain gradient beta c between the grid unit and the downstream grid unit, wherein the calculation formula is as follows:
Wherein: e c is the grid cell elevation; e x is the downstream grid cell elevation; A straight line distance between the grid unit and the downstream grid unit; when the downstream grid cell codes 0, 2,4, and 6, the value of ε is 1, otherwise it is 1.414;
the step 2 comprises the following substeps:
2.1, selecting a digital elevation model D s with resolution higher than D c, and dispersing grid units into a plurality of small grid units with side length L s;
2.2 calculating the terrain gradient beta s between the small grid units with the side length of L s in the grid units by adopting the methods in the steps 1.2 and 1.3;
2.3 calculating a first order origin moment of the terrain gradient beta s, upscaling to a calculation scale, quantifying the terrain fluctuation beta σ inside the grid unit, and the calculation formula is as follows:
Wherein: i is the number of a small grid unit with the side length L s inside the grid unit, and the number is from 1 to n; n is the number of small grid units with side length L s inside the grid units;
the step 3 comprises the following substeps:
3.1, using rainfall P and evaporation E as input, and calculating water flow q which can flow out freely in the grid unit by adopting a full-reservoir flow model and a linear reservoir formula;
3.2 dividing the water flow q into a water flow q c entering the downstream grid unit air-packing belt and a water flow q s discharged into the grid unit internal channel according to the ratio between beta c and beta s, and calculating the following formula:
qc+qs＝q；
2. A hydrographic model water flow along path allocation method taking into account terrain effects as claimed in claim 1, wherein: the step 4 comprises the following substeps:
4.1 the water flow q c is continuously flowed out after supplementing the air-packing belt water-shortage quantity of the downstream grid unit,
When w+pe+q c is less than or equal to WM, r=0;
When w+pe+q c > WM, r=pe+w+q c -WM;
wherein: WM is the water storage capacity of the tension water; w is tension water content; PE is rainfall after evaporation loss is deducted, namely net rain; r is the generated runoff amount;
the runoff amount R is converted into a water flow q b capable of flowing after being calculated by a water diversion source of a full-reservoir flow model and a linear reservoir method;
4.2, fast moving the water flow Q s between different grid units through the channels, solving the water flow Q through the following two formulas simultaneously to obtain the channel water flow Q, and then gradually accumulating to obtain the runoff process of the outlet of the river basin;
Wherein: a is the cross-sectional area of channel water flow, Q is the channel water flow; s f is the hydraulic gradient, and S o is the channel gradient; t is a time term, and the value is a calculation time interval; x is a space term and the value is the side length of the grid cell.
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