JP2010044048A - Method, system and program for analysis of underground water origin, recording medium, and method and unit for computing rainfall cultivation amount - Google Patents

Abstract

<P>PROBLEM TO BE SOLVED: To provide a method, system and program for analysis of an underground water origin, a recording medium, and a method and unit for computing a rainfall cultivation amount. <P>SOLUTION: A topographic surveying section 361 in an outflow rate computing section 36 divides a target area into a plurality of watersheds based on topographic data and conducts a topographic survey in the divided watersheds. A statistics processing section 362 extracts a plurality of factors having correlations with flowability of water out of results of the topographic survey. An outflow index determining section 363 calculates outflow indexes of the divided watersheds out of the plurality of factors. An outflow rate estimation section 364 derives a regression formula out of correlations between the outflow indexes of part of the watersheds and measured outflow rates therein, and calculates the outflow rates in the divided watersheds out of the derived regression formula and the outflow indexes of the divided watersheds. A rainwater cultivation amount computing section 32a calculates the rainfall cultivation amount based on the calculated outflow rates. <P>COPYRIGHT: (C)2010,JPO&INPIT

Description

  The present invention relates to a groundwater origin analysis method, a groundwater origin analysis system, a groundwater origin analysis program, and a recording medium using satellite image data.

  Groundwater origin analysis refers to the calculation of the area (hereinafter referred to as “recharge point”) where surface water from groundwater penetrates the ground and is used as groundwater. It means calculating that it is groundwater at a remote point. The calculation is performed by calculating which route the flow has reached until the groundwater reaches a point away from the recharge point. Such calculation of the origin of groundwater is regarded as important in managing the quality of groundwater. In such groundwater origin analysis, since it is necessary to analyze across multiple water systems, a survey covering a wide range is performed, and the amount of information handled is enormous. In addition, when the topography of the target area is indicated by a three-dimensional model and calculation processing is performed based on the model, approximation processing is performed for the purpose of simplifying arithmetic processing and the like in order to repeatedly perform processing with different condition settings. It has been broken. (For example, see Non-Patent Document 1)

Toyama et al., “Precipitation infiltration and underground water runoff model at the Tomitaka Mine, Miyazaki Prefecture”, Abstracts of the 2006 Autumn Lecture Meeting of the Japanese Groundwater Society, 2006.

When obtaining information used for groundwater origin analysis, it is necessary to obtain as accurate information as possible under limited conditions. The condition is that it is difficult to quantitatively measure the amount of osmotic water. The amount of evapotranspiration should change depending on the conditions of vegetation and the ground surface. In addition, information on a wide area is required. Therefore, how to improve the accuracy of the model obtained by approximation is the key to performing an accurate calculation process.
However, in the analysis of groundwater origin according to Non-Patent Document 1, the amount of infiltrated water is calculated by using a value obtained by uniformly multiplying the rainfall by a predetermined ratio based on experience as an approximate value of the amount of infiltrated water. It was. Even if there is the same amount of rainfall, the amount of penetration actually varies depending on the land use situation. Therefore, there is a problem that the approximate value of the actual permeated water amount cannot approximate the actual value, and the approximation accuracy affects the calculation result.
Moreover, there is a problem that the validity determination of the recharge point indicated by the obtained calculation result is derived from the result obtained by one calculation and cannot be verified.

The present invention has been made to solve the above problems, and its purpose is to provide a groundwater origin analysis method, a groundwater origin analysis system, a groundwater origin analysis program, a recording medium, a rainfall recharge amount calculation method, and a rain recharge amount calculation unit. There is to do.

  In order to solve the above problem, the present invention provides a rain recharge amount calculation method for calculating a rain recharge amount from an outflow amount, a precipitation amount, and an evapotranspiration amount, and the step of calculating the outflow amount includes a topography Dividing the target area into a plurality of basins from the data, and extracting a plurality of factors having a correlation between the first step of measuring topography in the divided basins and the ease of water flow from the topographic measurement results And a third step of calculating the outflow index of the divided basin from the plurality of factors, and a regression equation from a correlation between the outflow index of a part of the basin and the actually measured outflow amount. A rain recharge amount calculation method comprising: a fourth step of deriving; and a fifth step of calculating an outflow amount of the divided basin from the derived regression equation and an outflow index of the divided basin. .

  Further, in the present invention according to the above-mentioned invention, the third step extracts a first factor having a positive correlation with the ease of water flow and a second factor having a negative correlation with the ease of water flow. , Calculating a factor score for each factor of the divided basin, classifying the divided basin into a predetermined number of groups for each factor according to the calculated factor score, and each group for each factor A predetermined score is assigned to the basin, and an outflow index of the divided basin is calculated according to the given score and the contribution ratio of each factor.

  Further, the present invention divides the target area into a plurality of basins from the terrain data, and a plurality of terrain measurement units that perform terrain measurement in the divided basins and a plurality of correlations between the terrain measurement results and the ease of water flow. A statistical processing unit that extracts factors; an outflow index determination unit that calculates an outflow index of the divided basin from the plurality of factors; an outflow index of a part of the basin and the measured outflow amount An outflow amount calculation unit comprising a regression equation derived from the correlation and an outflow amount estimation unit that calculates the outflow amount of the divided basin from the derived regression equation and the outflow index of the divided basin is calculated The rain recharge amount calculation unit calculates a rain recharge amount based on the amount of runoff.

  In the present invention, the outflow index determination unit extracts the first factor having a positive correlation with the ease of water flow and the second factor having a negative correlation with the ease of water flow. , Calculating a factor score for each factor of the divided basin, classifying the divided basin into a predetermined number of groups for each factor according to the calculated factor score, and each group for each factor A predetermined score is assigned to the basin, and an outflow index of the divided basin is calculated according to the given score and the contribution ratio of each factor.

  Further, according to the present invention, the ion concentration determination processing unit calculates the origin of groundwater from the degree of coincidence of the ion concentration ratios in the ion concentration data at a plurality of points stored in the storage unit, and the isotope ratio determination processing unit stores the storage unit. The step of calculating the recharge height from the isotope ratio coincidence in the isotope ratio data stored in the multiple locations, and the evaporation for each region in the vegetation area satellite image data stored in the storage unit by the evapotranspiration calculation unit The step of calculating the amount of spatter, the step of calculating the amount of runoff by the runoff amount calculating unit, and the amount of rainfall recharge calculating unit calculating the amount of seepage water from the amount of evapotranspiration, the amount of precipitation stored in the storage unit, and the amount of runoff The step of calculating the position of the groundwater level 0 m for each region from the satellite image data indicating the river area stored in the storage unit, and the total head calculation processing unit Point elevation information A groundwater origin analysis method comprising: a step of calculating a water head value of the region from, and a step of calculating a groundwater transfer route and a transition time from a distribution of the water head value by a groundwater transfer route / transfer time calculation processing unit, The step of calculating the amount of runoff correlates between the first step of dividing the target area into a plurality of basins from the terrain data and measuring the terrain in the divided basins and the ease of water flow from the terrain measurement results. A second step of extracting a plurality of factors having the above, a third step of calculating an outflow index of the divided basin from the plurality of factors, and an outflow index of a part of the basin A fourth step of deriving a regression equation from the correlation with the outflow amount; a fifth step of calculating the outflow amount of the divided basin from the derived regression equation and the outflow index of the divided basin; Characterized by having It is a groundwater origin analysis how to.

  The present invention also provides an ion concentration determination processing unit for calculating the origin of groundwater from the degree of coincidence of ion concentration ratios in ion concentration data stored at a plurality of points stored in a storage unit, and isotopes at a plurality of points stored in the storage unit An isotope ratio determination processing unit that calculates the recharge height from the degree of coincidence of the isotope ratios in the ratio data, and an evapotranspiration calculation unit that calculates the evapotranspiration amount for each region from the satellite image data of the vegetation area stored in the storage unit An outflow amount calculation unit for calculating an outflow amount, a rain recharge amount calculation unit for calculating an infiltration water amount from the evapotranspiration, a precipitation amount stored in the storage unit, and the outflow amount, and a storage unit. Total head calculation to calculate the head value of the area from the pressure head 0 m setting unit that sets the position of the groundwater level 0 m for each area from the satellite image data indicating the river area, and the amount of seepage water and the altitude information of each point A processing unit; A groundwater transfer route / transition time calculation processing unit that calculates a groundwater transfer route and a transfer time from the distribution of peak values, the runoff amount calculating unit comprising a plurality of target areas from terrain data From the plurality of factors, a terrain measurement unit that divides the river basin and performs terrain measurement in the divided basin, a statistical processing unit that extracts a plurality of factors having a correlation between water flow easiness from the terrain measurement result, and An outflow index determination unit that calculates an outflow index of the divided basin, and derives a regression equation from a correlation between the outflow index of a part of the basin and the measured outflow amount, and the derived regression equation And an outflow amount estimating unit for calculating an outflow amount of the divided basin from an outflow index of the divided basin.

  The present invention also includes a step of calculating a groundwater origin from a degree of coincidence of ion concentration ratios in ion concentration data stored at a plurality of points stored in a storage unit in a computer of the groundwater origin analysis system, and a plurality of storage units stored in the storage unit. Calculating the recharge height from the isotope ratio coincidence in the isotope ratio data of the point, calculating the evapotranspiration for each region from the satellite image data of the vegetation area stored in the storage unit, Calculating the amount of seepage water from the step of calculating, the amount of evapotranspiration, the amount of precipitation stored in the storage unit, and the amount of runoff, and the satellite image data indicating the river area stored in the storage unit for each region. Setting the position of the groundwater level of 0 m, calculating the water head value of the area from the amount of seepage water and the altitude information of each point, and the distribution of the water head value And a step of calculating a groundwater transfer route and a transfer time, wherein the step of calculating the amount of runoff divides the target area into a plurality of basins from topographic data, and the divided basins A first step of performing topographic measurement in step 2, a second step of extracting a plurality of factors having a correlation with the ease of water flow from the topographic measurement results, and outflow of the divided basin from the plurality of factors A third step of calculating an index, a fourth step of deriving a regression equation from a correlation between an outflow index of a part of the basin and the measured outflow amount, the derived regression equation and the And a fifth step of calculating an outflow amount of the divided basin from an outflow index of the divided basin.

  Further, the present invention is a computer-readable recording medium that records the above-described program to be executed by a computer in a groundwater origin analysis system.

  In addition, the present invention has means according to the invention described below, and calculates the amount of osmotic water corrected by the calculated value of the evapotranspiration calculated based on the satellite image data of the vegetation area stored in the storage unit. The groundwater origin analysis method is characterized in that the transition route and the transition time of groundwater are calculated from the distribution of the head value based on the amount of osmotic water.

  Further, according to the present invention, the ion concentration determination processing unit calculates the origin of groundwater from the degree of coincidence of the ion concentration ratios in the ion concentration data at a plurality of points stored in the storage unit, and the isotope ratio determination processing unit stores the storage unit. The step of calculating the recharge height from the isotope ratio coincidence in the isotope ratio data stored in the multiple locations, and the evaporation for each region in the vegetation area satellite image data stored in the storage unit by the evapotranspiration calculation unit A step of calculating the amount of spray, a step of calculating the amount of osmotic water from the evapotranspiration amount and the value of precipitation stored in the storage unit, and a pressure head 0 m setting unit stored in the storage unit A step of calculating the position of the groundwater level 0 m for each region from satellite image data indicating a river region, and a step of calculating a head value of the region from the amount of seepage water and altitude information at each point by a total head calculation processing unit. , Groundwater transfer A step in which the road-shift time calculation processing unit calculates the groundwater migration route and transit time from the distribution of the water head value, a groundwater origin analysis method, which comprises a.

  The present invention also provides an ion concentration determination processing unit for calculating the origin of groundwater from the degree of coincidence of ion concentration ratios in ion concentration data stored at a plurality of points stored in a storage unit, and isotopes at a plurality of points stored in the storage unit An isotope ratio determination processing unit that calculates the recharge height from the degree of coincidence of the isotope ratios in the ratio data, and an evapotranspiration calculation unit that calculates the evapotranspiration amount for each region from the satellite image data of the vegetation area stored in the storage unit A rain recharge amount calculation unit for calculating an infiltration water amount from the evapotranspiration amount and a precipitation value stored in the storage unit, and a groundwater level for each region from satellite image data indicating a river area stored in the storage unit A pressure head 0m setting section for setting a position of 0 m, a total head calculation processing section for calculating a head value of the area from the amount of osmotic water and elevation information at each point, a groundwater transfer route and a transition from the distribution of the head value Time And groundwater movement path-shift time calculation processing unit for output, a groundwater origin analysis system, characterized in that it comprises a.

  The present invention also includes a step of calculating a groundwater origin from a degree of coincidence of ion concentration ratios in ion concentration data stored at a plurality of points stored in a storage unit in a computer of the groundwater origin analysis system, and a plurality of storage units stored in the storage unit. Calculating the recharge height from the isotope ratio coincidence in the isotope ratio data of the point, calculating the evapotranspiration for each region from the satellite image data of the vegetation area stored in the storage unit, and the evapotranspiration Calculating the amount of seepage water from the amount and the value of precipitation stored in the storage unit; setting the position of the groundwater level 0 m for each region from satellite image data indicating the river area stored in the storage unit; The step of calculating the head value of the region from the amount of osmotic water and the altitude information of each point, and calculating the groundwater transfer route and the transfer time from the distribution of the head value A groundwater origin analysis program, characterized in that to execute a step, the.

  Further, the present invention is a computer-readable recording medium that records the above-described program to be executed by a computer in a groundwater origin analysis system.

(1) According to the present invention, the rain recharge amount calculation method calculates the rain recharge amount from the outflow amount, the precipitation amount, and the evapotranspiration amount. The first step in calculating the outflow amount divides the target area into a plurality of basins from the terrain data, and performs terrain measurement in the divided basins. In the second step, a plurality of factors having a correlation with the ease of water flow are extracted from the terrain measurement result. In the third step, the outflow index of the basin divided from the plurality of factors is calculated. In the fourth step, a regression equation is derived from the correlation between the outflow index of a part of the basin and the actually measured outflow amount. In the fifth step, the outflow amount of the divided basin is calculated from the derived regression equation and the outflow index of the divided basin.
Thereby, in the calculation of rainfall recharge, the amount of rain recharge can be derived based on the index indicated by the features of each terrain in the divided basin, not on the assumption of runoff.

(2) According to the present invention, in the above invention, the third step includes a first factor having a positive correlation with the ease of water flow and a second factor having a negative correlation with the ease of water flow. And calculate the factor score for each factor of the divided basin, classify the divided basin into the number of groups set in advance for each factor according to the calculated factor score, each for each factor A preset score is assigned to each group, and the outflow index of the basin divided according to the assigned score and the contribution rate of each factor is calculated.
As a result, it is possible to extract two factors indicating the ease of water flow, to calculate the runoff index of the basin calculated based on those factors, and to derive the amount of rainfall recharge according to the characteristics of the basin .

(3) According to the present invention, the terrain measurement unit divides the target area into a plurality of basins from the terrain data, and performs terrain measurement in the divided basins. The statistical processing unit extracts a plurality of factors having a correlation with the ease of water flow from the topographic measurement result. The outflow index determination unit calculates the outflow index of the divided basin from a plurality of factors. The runoff estimator derives a regression equation from the correlation between the runoff index of a part of the basin and the measured runoff, and the basin of the basin divided from the derived regression equation and the runoff index of the divided basin Based on the outflow amount output by the outflow amount estimation unit for calculating the outflow amount, the rain recharge amount calculation unit calculates the rain recharge amount.
As a result, the rainfall recharge calculating unit derives the rain recharge based on the index indicated by the characteristics of each terrain in the divided basin, not on the assumption of runoff in calculating the rain recharge. be able to.

(4) According to the present invention, the runoff index determination unit in the rainfall recharge calculating unit has the first factor having a positive correlation with the ease of water flow and the second factor having a negative correlation with the ease of water flow. Factors are extracted, and a factor score for each factor of the divided watershed is calculated. Further, the outflow index determination unit classifies the basin divided according to the calculated factor score into a group number set in advance for each factor, and assigns a preset score to each group for each factor, Calculate the outflow index of the divided basin according to the score given and the contribution rate of each factor.
As a result, the rainfall recharge calculating unit derives the rain recharge based on the index indicated by the characteristics of each terrain in the divided basin, not on the assumption of runoff in calculating the rain recharge. be able to.

(5) According to the present invention, in the groundwater origin analysis method, the ion concentration determination processing unit calculates the groundwater origin from the degree of coincidence of the ion concentration ratios in the ion concentration data at a plurality of points stored in the storage unit. The isotope ratio determination processing unit calculates the recharge height from the degree of coincidence of the isotope ratios in the isotope ratio data at a plurality of points stored in the storage unit. The evapotranspiration calculating unit calculates the evapotranspiration amount for each region in the vegetation area satellite image data stored in the storage unit. The outflow amount calculation unit calculates the outflow amount. A rainfall recharge amount calculation unit calculates an infiltration water amount from the evapotranspiration amount, the precipitation amount stored in the storage unit, and the outflow amount. The pressure head 0 m setting unit calculates the position of the groundwater level 0 m for each region from the satellite image data indicating the river area stored in the storage unit. The total head calculation processing unit calculates the head value of the region from the amount of seepage water and the altitude information at each point. The groundwater transfer route / transfer time calculation processing unit calculates the groundwater transfer route and the transfer time from the distribution of the head value.
In addition, in the calculation of the outflow amount, the first step divides the target area into a plurality of basins from the terrain data, and performs terrain measurement in the divided basins. In the second step, a plurality of factors having a correlation with the ease of water flow are extracted from the terrain measurement result. A third step calculates an outflow index of the divided basin from the plurality of factors. In the fourth step, a regression equation is derived from the correlation between the outflow index of a part of the basin and the actually measured outflow amount. In the fifth step, the outflow amount of the divided basin is calculated from the derived regression equation and the outflow index of the divided basin.

  In addition, by calculating the amount of osmotic water, which is difficult to measure directly, based on satellite image data in the vegetation area, deviation from the approximate model caused by changes in evapotranspiration due to vegetation conditions and ground surface conditions Can be reduced. In addition, information on a wide area is obtained by using satellite image data. And in the calculation of rainfall recharge, it is possible to improve the accuracy of the model obtained by approximation by performing correction according to the situation for each point in the divided basin rather than calculation assuming runoff. It is possible to calculate the accurate groundwater transfer route and transfer time. In addition, the validity of the recharge point shown by the calculation results of the groundwater transfer route and the transfer time calculation process is verified by associating and verifying the results calculated in multiple processes. Can be confirmed.

(6) In the groundwater origin analysis system, the ion concentration determination processing unit calculates the groundwater origin from the degree of coincidence of the ion concentration ratios in the ion concentration data at a plurality of points stored in the storage unit. The isotope ratio determination processing unit calculates the recharge height from the degree of coincidence of the isotope ratios in the isotope ratio data stored in the storage unit. The evapotranspiration calculating unit calculates the evapotranspiration amount for each region from the satellite image data of the vegetation area stored in the storage unit. The outflow amount calculation unit calculates the outflow amount. The recharge amount calculation unit calculates the amount of seepage water from the evapotranspiration amount, the precipitation amount stored in the storage unit, and the outflow amount. The pressure head 0 m setting unit sets the position of the groundwater level 0 m for each region from the satellite image data indicating the river area stored in the storage unit. The total head calculation processing unit calculates the head value of the area from the amount of infiltrated water and the altitude information at each point. The groundwater transfer route / transfer time calculation processing unit calculates the groundwater transfer route and the transfer time from the distribution of the head value.
Further, the outflow amount calculation unit divides the target area into a plurality of basins from the terrain data, and performs terrain measurement in the divided basins. The statistical processing unit extracts a plurality of factors having a correlation with the ease of water flow from the topographic measurement result. An outflow index determination unit calculates an outflow index of the divided basin from a plurality of factors. An outflow estimation unit derives a regression equation from the correlation between the outflow index of a part of the basin and the measured outflow amount, and the divided equation is derived from the derived regression equation and the outflow index of the divided basin. Calculate the amount of runoff in the basin.

  In this way, the amount of seepage water that is difficult to measure directly is calculated based on satellite image data in the vegetation area, thereby reducing deviations in the evapotranspiration from the approximate model caused by changes in the vegetation situation and the ground surface situation. it can. In addition, information on a wide area is obtained by using satellite image data. And in the calculation of rainfall recharge, it is possible to improve the accuracy of the model obtained by approximation by performing correction according to the situation for each point in the divided basin rather than calculation assuming runoff. It is possible to calculate the accurate groundwater transfer route and transfer time. In addition, the validity of the recharge point shown by the calculation results of the groundwater transfer route and the transfer time calculation process is verified by associating and verifying the results calculated in multiple processes. Can be confirmed.

According to this invention, the groundwater origin analysis method calculates the amount of osmotic water corrected by the calculated value of the evapotranspiration calculated based on the satellite image data of the vegetation area, and calculates the groundwater from the distribution of the head value based on the amount of osmotic water. The transition route and the transition time are calculated.
In this way, by setting the amount of infiltrated water that is difficult to measure directly based on satellite image data in the vegetation area, the evapotranspiration amount is deviated from the approximate model caused by changes in the vegetation situation and the ground surface condition. Can be reduced. In addition, information on a wide area is obtained by using satellite image data. And by performing the correction | amendment according to the condition for every point, the accuracy of the model calculated | required by approximation can be raised, and it becomes possible to perform the calculation process of an exact groundwater transfer route and transfer time.

According to the present invention, in the groundwater origin analysis method, the ion concentration determination processing unit calculates the groundwater origin from the degree of coincidence of the ion concentration ratios in the ion concentration data at a plurality of points stored in the storage unit. The isotope ratio determination processing unit calculates the recharge height from the degree of coincidence of the isotope ratios in the isotope ratio data at a plurality of points stored in the storage unit. The evapotranspiration calculating unit calculates the evapotranspiration amount for each region in the vegetation area satellite image data stored in the storage unit. The rainfall recharge amount calculation unit calculates the amount of infiltrated water from the evapotranspiration amount and the precipitation value stored in the storage unit. The pressure head 0 m setting unit calculates the position of the groundwater level 0 m for each region from the satellite image data indicating the river area stored in the storage unit. The total head calculation processing unit calculates the head value of the region from the amount of seepage water and the altitude information at each point. The groundwater transfer route / transfer time computation processing unit calculates the groundwater transfer route and the transfer time from the distribution of the head value.
In addition, by calculating the amount of osmotic water, which is difficult to measure directly, based on satellite image data in the vegetation area, deviation from the approximate model caused by changes in evapotranspiration due to vegetation conditions and ground surface conditions Can be reduced. In addition, information on a wide area is obtained by using satellite image data. And by performing the correction according to the situation for each point, it is possible to increase the accuracy of the model obtained by approximation, and it is possible to accurately calculate the groundwater transfer route and the transfer time. In addition, the validity of the recharge point shown by the calculation results of the groundwater transfer route and the transfer time calculation process is verified by associating and verifying the results calculated in multiple processes. Can be confirmed.

It is a block diagram which shows the groundwater origin analysis system by this embodiment. It is a figure which shows the ion concentration analysis in the same embodiment. It is a figure which shows the water quality analysis in the same embodiment. It is a figure which shows the isotope ratio analysis in the same embodiment. It is a figure (the 1) of isotope ratio analysis in the same embodiment. It is a figure (the 2) of isotope ratio analysis in the same embodiment. It is a figure (the 3) of isotope ratio analysis in the same embodiment. It is a figure (the 4) of the isotope ratio analysis in the same embodiment. It is a figure (the 1) which shows the remote sensing information in the same embodiment. It is a figure (the 2) which shows the remote sensing information in the same embodiment. It is a figure which shows the difference information calculated | required from the remote sensing information in the embodiment. It is a figure which shows the land use classification calculated | required from the remote sensing information in the embodiment. It is a figure which shows the amount of evapotranspiration calculated | required from the remote sensing information in the same embodiment. It is a figure which shows the surface water surface in the same embodiment. It is a figure which shows the result of having set geological information about each point in the embodiment. It is a figure which shows the total head distribution in the same embodiment. It is a figure which shows the actual measurement data of the groundwater surface elevation in the embodiment. It is a figure which shows the flow of groundwater in the same embodiment. It is a figure which shows the transfer route of groundwater in the same embodiment. It is a flowchart which shows the groundwater origin analysis process in the embodiment. It is a figure which shows the data structure of the data used for the ion concentration analysis process in the embodiment. It is a flowchart which shows the ion concentration analysis process in the embodiment. It is a figure which shows the data structure of the data used for the isotope ratio analysis process in the embodiment. It is a flowchart which shows the isotope ratio analysis process in the embodiment. It is a figure which shows the data structure of the data used for the evapotranspiration calculation process from the remote sensing information in the embodiment. It is a flowchart which shows the evapotranspiration calculation process in the embodiment. It is a figure which shows the data structure of the data used for the rainfall recharge amount calculation process in the embodiment. It is a flowchart which shows the rainfall amount calculation process in the embodiment. It is a figure which shows the data structure of the data used for the pressure head 0m setting process in the embodiment. It is a flowchart which shows the pressure head 0m setting process in the embodiment. It is a figure which shows the data structure of the data used for the total head value calculation process in the embodiment. It is a flowchart which shows the total head value calculation process in the embodiment. It is a figure which shows the data structure of the data used for the groundwater transfer path | route / time calculation process in the embodiment. It is a figure which shows the flowchart which shows the groundwater transfer path | route / time calculation process in the embodiment. It is a block diagram which shows the groundwater transfer calculation process part by this embodiment. It is a figure which shows the basin by which the division process in the same embodiment was carried out. It is a figure which shows the result of having statistically processed the topographic measurement data in the same embodiment. It is a figure which shows the result of having statistically processed the topographic measurement data in the same embodiment. It is a figure which shows the result of having statistically processed the topographic measurement data in the same embodiment. It is a figure which shows the result of having statistically processed the topographic measurement data in the same embodiment. It is a figure which shows the result of having statistically processed the topographic measurement data in the same embodiment. It is a figure which shows the result of having statistically processed the topographic measurement data in the same embodiment. It is a figure which shows the factor score distribution of the divided basin in the same embodiment. It is a figure which shows the factor score distribution of the divided basin in the same embodiment. FIG. 45 is a supplementary explanatory diagram of FIG. 44. It is a figure which shows distribution of the outflow parameter | index of the divided basin in the same embodiment. It is a figure which shows distribution of the specific flow rate actual value of the divided basin in the embodiment. It is a graph which shows the relationship between the outflow parameter | index and the specific flow rate actual value in the same embodiment. It is a figure which shows distribution of the specific flow rate estimated value of the divided basin in the embodiment. It is a graph which shows the relationship between the altitude value and the amount of rainfall in the embodiment. It is a figure which shows distribution of the correction | amendment rainfall amount of the divided basin in the same embodiment. It is a flowchart which shows the rainfall amount calculation process in the embodiment. It is a figure which shows the data structure of the data used for the topography measurement process in the embodiment. It is a flowchart which shows the topography measurement process in the embodiment. It is a figure which shows the data structure of the data used for the statistical process in the embodiment. It is a figure which shows the data structure of the data used for the statistical process in the embodiment. It is a flowchart which shows the statistical process in the embodiment. It is a figure which shows the data structure of the data used for the outflow index calculation process in the embodiment. It is a figure which shows the data structure of the data used for the outflow index calculation process in the embodiment. It is a flowchart which shows the outflow index calculation process in the embodiment. It is a figure which shows the data structure of the data used for the outflow amount estimation process in the embodiment. It is a flowchart which shows the outflow amount estimation process in the embodiment. It is a figure which shows the data structure of the data used for the outflow amount estimation process in the embodiment. It is a flowchart which shows the outflow amount estimation process in the embodiment. It is a figure which shows the data structure of the data used for the precipitation estimation process in the embodiment. It is a flowchart which shows the precipitation amount estimation process in the embodiment. It is a figure which shows the data structure of the data used for the rainfall recharge amount calculation process in the embodiment. It is a flowchart which shows the rainfall amount calculation process in the embodiment. It is a figure which shows the relationship between runoff, precipitation, evapotranspiration, and rainfall recharge.

Hereinafter, a groundwater origin analysis system 100 according to an embodiment of the present invention will be described with reference to the drawings.
FIG. 1 is a block diagram showing a groundwater origin analysis system 100 according to this embodiment.
This figure shows a groundwater origin analysis system 100 and an information input system 200 that provides information used in the processing of the groundwater origin analysis system 100.
The groundwater origin analysis system 100 is a groundwater origin analysis system that performs arithmetic processing based on various information input from the information input system 200 and calculates a recharge point that is a source of groundwater at the point. The recharge point is a place where the water that has become surface water by rainfall penetrates the ground and becomes groundwater. The altitude at that point is called dependent altitude. Then, the groundwater moves according to the flow of groundwater starting from the recharge point.
Further, in the calculation of the recharge point by the groundwater origin analysis system 100, a route until the groundwater that reaches a predetermined position / depth reaches the point is calculated, and the base point of the route is calculated as a recharge point. The groundwater origin analysis system 100 is a system that calculates the time from rainfall until reaching a predetermined position and depth.

  The information input system 200 is an ion / water quality information system (ion / water quality information data) 210 that provides ion concentration / water quality information detected from river water or groundwater, and isotope ratio information detected from river water or groundwater. Isotope information system (isotope information data) 220, a remote sensing system 231 that provides image information taken by an artificial satellite, a rainfall information system 232 that provides rainfall at each location, and topographic elevation information at each location A map information system 233 that provides latitude and longitude and altitude, and a geological information system 234 that provides information related to geology.

The groundwater origin analysis system 100 includes an arithmetic processing unit 110, an input processing unit 40, a control storage processing unit 50, a storage unit 70, an output processing unit 80, and a display unit 90.
In the groundwater origin analysis system 100, the arithmetic processing unit 110 performs various arithmetic processes in the groundwater origin analysis system 100. The arithmetic processing unit 110 in the groundwater origin analysis system 100 includes an ion concentration water quality information determination processing unit 10, an isotope ratio determination processing unit 20, and a groundwater transfer calculation processing unit 30. In the arithmetic processing unit 110, the ion concentration water quality information determination processing unit 10 determines the correlation of each of the ion concentration / water quality information detected from the sample such as river water or groundwater. The ion concentration water quality information determination processing unit 10 is a determination processing unit that can handle determination results from samples with high similarity as a group. The isotope ratio determination processing unit 20 specifies the altitude of the recharge point that is the origin of the groundwater, that is, the recharge height, based on the isotope ratio information detected from the sample of river water or groundwater. The isotope ratio determination processing unit 20 is a determination processing unit that can handle determination results from samples having high water source similarity as a group.

  The groundwater transfer calculation processing unit 30 is recharged as groundwater at the point where it rains, and calculates the transition route and transition time until it reaches the groundwater as the groundwater by the topography, altitude difference and environment of the groundwater flow. This is a determination processing unit. The groundwater transfer calculation processing unit 30 includes an evapotranspiration calculation unit 31, a rainfall recharge calculation unit 32, a pressure head 0m setting unit 33, a total head calculation processing unit 34, and a groundwater transfer route / transfer time calculation processing unit 35. In the groundwater transfer calculation processing unit 30, the evapotranspiration calculating unit 31 performs a calculation process based on image data taken from an artificial satellite, and calculates a possible evapotranspiration amount at each point. The rainfall recharge calculating unit 32 performs a calculation process based on the information on the possible evapotranspiration at each point and the rainfall at each point, and calculates the rain recharge at each point. The pressure head 0 m setting unit 33 performs arithmetic processing based on image data taken from an artificial satellite and information on latitude and longitude and altitude, and a point where the pressure head indicates 0 m, that is, groundwater becomes surface water as a river. Set the point where it appears. The total head calculation processing unit 34 calculates the total head value information by calculating based on the information on the point where the rain recharge amount and the pressure head at each point show 0 m, the latitude longitude and the altitude information. The groundwater transfer route / transfer time calculation processing unit 35 performs calculation processing based on the total head value information of each point to calculate the groundwater transfer route and the transfer time.

  The input processing unit 40 receives information from the connected information input system 200. The input processing unit 40 records information input through the processing of the control storage processing unit 50 in each storage unit allocated to the storage unit 70. As information input from the information input system 200, either information recorded on a computer-readable medium or information input by communication processing performed via a communication line can be selected. The input processing unit 40 includes an input unit such as a mouse and a keyboard, performs processing for detecting information input from the input unit, and inputs the detected result to the control storage processing unit 50.

  The control storage processing unit 50 discriminates instructions from each processing unit in the groundwater origin analysis system 100, outputs a response to the instructions, controls each processing unit, records information in the storage unit 70, and stores the information in the storage unit 70. Reference information. The storage unit 70 is a storage unit configured by an HDD (Hard disk drive), a semiconductor memory, or the like, and recording and reference are performed in accordance with an instruction from the control storage processing unit 50. The output processing unit 80 creates a display screen for selecting an input processing instruction required for each computation process, creates a display screen for displaying computation results, and displays information about the created screen on the display unit 90. Output to. The display unit 90 performs display processing for displaying the screen information input from the output processing unit 80. The display unit 90 is a display unit using display elements of various display methods such as a CRT (Cathode Ray Tube), an LCD (Liquid Crystal Display), a PDP (Plasma Display Panel), and an EL (Electro-Luminescence) display. Also good.

  The groundwater origin analysis system 100 includes a CPU (Central Processing Unit), a RAM (Random Access Memory), a ROM (Read Only Memory), a HDD (Hard Disk Drive), an I / O (Input / Output), and the like. The CPU that executes the arithmetic processing uses the RAM as a temporary work area, a setting storage area, or as a program area, while appropriately executing the basic program written in the ROM, via the I / O It controls connected external devices, internal devices, etc. Furthermore, the groundwater origin analysis system 100 includes an HDD as a storage area inside the apparatus, and stores information such as processing programs, information as various tables, and processing results. Used as

Next, functions of various processes of the groundwater origin analysis system 100 will be described with reference to the drawings.
In the groundwater origin analysis system 100, the arithmetic processing unit 110 performs various arithmetic processes in the groundwater origin analysis system 100. The ion concentration water quality information determination processing unit 10 in the arithmetic processing unit 110 refers to the following information among the ion concentration / water quality information detected from the river water or groundwater provided from the ion / water quality information data 210 as a sample. To do.
As the ion concentration analysis, each ion concentration classified into the following six is analyzed. That is, sulfate ions (SO ₄ ²⁻ ), bicarbonate ions (HCO ₃ ⁻ ), chlorine ions (Cl ⁻ ), calcium ions (Ca ²⁺ ), magnesium ions (Mg ²⁺ ), and sodium and potassium ions (Na ⁺ and K) ⁺ ). The ion concentration water quality information determination processing unit 10 can perform trend analysis indicating similarity of the ratio of ion concentrations by the arithmetic processing by performing arithmetic processing by the principal component analysis technique based on the ion concentration data.

FIG. 2 is a diagram illustrating an example of ion concentration analysis.
In order to visually compare the tendency of the ratio of these ion concentrations shown by the samples at a plurality of locations, a technique called a water quality diagram is used. The detected ions are classified into six. The classification includes sulfate ions (SO ₄ ²⁻ ), bicarbonate ions (HCO ₃ ⁻ ), chlorine ions (Cl ⁻ ) as anions, calcium ions (Ca ²⁺ ) and magnesium ions (Mg ²⁺ ) as cations. ), Sodium ions and potassium ions (Na ⁺ and K ⁺ ). According to the classification, anions are arranged on the left and cations on the right as shown. The horizontal axis of the graph shown in this figure indicates the value of ion concentration. The shape indicated by the hexagons plotted on the graph according to the concentration of each ion and drawn by connecting the plot points shows the characteristics of the amount of ions contained in the water. It can be determined that samples having similar hexagonal shapes are likely to be groundwater of the same water system. As shown in FIGS. (A) and (b), water having different hexagonal features can be determined as water from different water systems. The ion concentration water quality information determination processing unit 10 can also create a water quality diagram with reference to the stored ion concentration data.

In addition, as an example of water quality information analysis, an example of analyzing electrical conductivity and water temperature is shown.
Fig.3 (a) is a graph which shows the relationship between the electrical conductivity obtained by analyzing each sample from the same water system, and the altitude which extract | collected the sample. The horizontal axis of this graph represents electric conductivity (μS (micro Siemens) / cm)), and the vertical axis represents altitude (m). As shown in this graph, in the case of samples using the same water system, the higher the altitude, the lower the electric conductivity, and the lower the altitude, the higher the electric conductivity. That is, while the sample water sampled at a low altitude is moving underground, the components in the ground constituting the route are dissolved and the ionization tendency is increased. The white circle (◯) mark shown in the figure shows an example in which the electrical conductivity obtained by analyzing a specific groundwater is plotted on a graph showing a known measurement result. In this example, since the position of the white circle (◯) is located within the range of variation indicated by each sample, it can be determined that the groundwater is from the same water system.
FIG. 3B is a graph showing the relationship between water temperature and altitude. The horizontal axis of this graph indicates the water temperature (° C.), and the vertical axis indicates the altitude (m). The sample shown in this graph is not limited to a specific water system, but shows the water temperature measured in groundwater and spring water flowing through multiple mountains. In this graph, when samples from the same mountain system are extracted, the sample tends to vary within a range that can be approximated by linearity. This straight line is called geothermal gradient. The two straight lines (solid line and broken line) shown in this figure indicate ground temperature gradients due to different mountain systems, and the water system is determined depending on which ground temperature gradient is correlated.
As described above, the ion concentration water quality information determination processing unit 10 in the arithmetic processing unit 110 determines each correlation from information obtained from the samples of groundwater and spring water, and determines the similarity as a group. Part.

The isotope ratio determination processing unit 20 in the arithmetic processing unit 110 performs determination based on the isotope ratio information detected from river water, groundwater, or the like, that is, the stable isotope ratio indicating the content of stable isotopes included in the sample. .
A stable isotope that is analyzed by the isotope ratio determination processing unit 20 will be described.
FIG. 4A shows an isotope based on hydrogen H. FIG. Compared to standard hydrogen H, deuterium ² H with one more neutron and tritium ³ H with two more neutrons are shown. Hydrogen H and deuterium ² H are stable isotopes, while tritium ³ H is a radioisotope with a half-life (12.3 years). A stable isotope is used as a tracer for water system determination because its content does not naturally decrease like a radioisotope.
FIG. 4B is a diagram showing the content of stable isotopes contained in general water.
As stable isotopes contained in water, stable isotopes related to hydrogen atoms and oxygen atoms constituting water are shown. This figure shows five stable isotopes of hydrogen H, deuterium ² H (D), oxygen ¹⁶ O, oxygen ¹⁷ O, and oxygen ¹⁸ O and their abundance ratios. As shown here, oxygen ¹⁸ O has a higher abundance ratio than other stable isotopes, and is suitable for a tracer used for groundwater source analysis. The stable isotope ratio of oxygen ¹⁸ O is shown as “δ ¹⁸ O”.
FIG. 5 is a graph showing the relationship between the stable isotope ratio (δ ¹⁸ O) of a specific water system and the altitude of the recharge location. The horizontal axis of this graph represents the stable isotope ratio (δ ¹⁸ O: ‰ (permil)), and the vertical axis represents the altitude (m). As shown by this graph, in the case of the same water system, the sample tends to vary in a range that can be approximated by the straightness indicated by the linearity. When the altitude is high, the content of stable isotopes tends to decrease.

Further, it is known that the stable isotope ratio changes according to the evaporation amount.
FIG. 6 is a graph showing the relationship between the amount of evaporation and the change in stable isotope ratio (δ ¹⁸ O). The horizontal axis of this graph represents the evaporation rate (% (percent)), and the vertical axis represents the stable isotope ratio (δ ¹⁸ O: ‰ (permil)). The two graphs shown in this graph show changes in stable isotope ratios when two different river waters are evaporated. The value which becomes the intercept of the vertical axis | shaft of this graph is different, and it shows that it is the water of different river water. Both graphs show the same tendency that the graphs rise to the right according to the evaporation amount. As shown in this figure, the value of the isotope ratio increases as the evaporation amount increases. That is, it shows that the contained ratio becomes high.

FIG. 7 is a graph showing the relationship between the stable isotope ratio (δ ¹⁸ O) and the elevation of the observed rainfall collection location. The horizontal axis of this graph represents the stable isotope ratio (δ ¹⁸ O: ‰ (permil)), and the vertical axis represents the altitude (m). This figure plots data of a plurality of samples, and based on the information of these measurement points, a straight line Eref2 (solid line) in consideration of a correction amount and a straight line Pref1 (dotted line) indicated by a linear equation based on linear regression analysis. Is shown. The tendency indicated by the straight line Pref1 indicates the tendency of the stable isotope ratio at the actual measurement point. This trend does not take into account changes in the stable isotope ratio due to evaporation from the time of rainfall until it is measured.
As shown in FIG. 6 described above, the stable isotope ratio increases as the evaporation proceeds. That is, the value indicated by the stable isotope amount indicated by the straight line EVP2 (solid line) is a stable isotope at the time when evaporation has progressed, and therefore it is necessary to correct the value by assuming the stable isotope ratio at the time of rainfall. . For example, a point P1 (stable isotope ratio: −10 ‰ (per mill), altitude: 1000 m) shown in the figure is measurement data of the collected groundwater. In order to correct this data, the new elevation value (2000 m) indicated by the straight line EVP2 for the same stable isotope ratio can be obtained by using the relationship indicated by the straight line EVP2 in consideration of the correction by evaporation. The straight line EVP2 is derived from the relationship considering the evaporation rate shown in FIG. That is, it is determined that there is a high possibility that water collected from groundwater at an altitude of 1000 m is infiltrated into groundwater by rainfall at an altitude of 2000 m.

FIG. 8 is a graph showing the relationship between stable isotope ratio (δ ¹⁸ O) and altitude in different water systems. The horizontal axis of this graph represents the stable isotope ratio (δ ¹⁸ O: ‰ (permil)), and the vertical axis represents the altitude (m). The three straight lines W1, W2, and W3 shown in this figure are graphs obtained by performing linear regression analysis from data of different aqueous samples. Different straight lines W1, W2, and W3 are obtained for each water system, and the water system can be determined using this feature. Also, similarity tendency analysis can be performed by performing arithmetic processing using a principal component analysis method based on stable isotope ratio data.

The groundwater transfer calculation processing unit 30 in the arithmetic processing unit 110 will be described with reference to the drawing.
In the groundwater transfer calculation processing unit 30, the evapotranspiration calculating unit 31 performs a calculation process for calculating a possible evapotranspiration amount at each point based on image data taken from an artificial satellite.
The image data taken from the artificial satellite is information obtained by detecting the intensity of reflected light from the ground surface filtered in two different wavelength ranges. The first wavelength region is a visible light region (hereinafter also referred to as “Band (band) 3” region), and the second wavelength region is a near-infrared region (hereinafter referred to as “Band (band) 4” region). It is also called.) By comparing the data of these two different wavelength regions, a normalized vegetation index (hereinafter referred to as “NDVI (Normalized Difference Vegetation Index)”) serving as an index indicating the degree of vegetation life at each point is calculated. NDVI is obtained from the following equation (1).

NDVI = (Bd4-Bd3) / (Bd4 + Bd3) (1)

In the formula (1), Bd3 is a value of reflectance (also referred to as “adbed”) indicated by the data of the Band3 region, and Bd4 is also a value of reflectance indicated by the data of the Band4 region.
FIG. 9 and FIG. 10 are diagrams showing two-dimensionally by calculating NDVI of each point based on the information indicating the difference in the reflectance of the ground surface photographed from the artificial satellite for each region. FIG. 9 shows the results measured at the leaf fall time, FIG. 10 shows the results measured at the leaf fall time, and the NDVI of each time was obtained from the reflectance information measured by changing the photographing time. is there. Each relationship is shown in Formula (2) and Formula (3) based on Formula (1).

NDVI (deciduous time) =
(Bd4 (deciduous leaf) −Bd3 (deciduous leaf)) / (Bd4 (deciduous leaf) + Bd3 (deciduous leaf)) (2)

  In Formula (2), NDVI (falling time) is the vegetation life degree (NDVI) of the falling time, Bd3 (falling) is the reflectance in the visible light region (Band3), and Bd4 (falling) is near red of the falling time. The reflectance of an external light area (Band4) is shown.

NDVI (leafing time) =
(Bd4 (leafing) −Bd3 (leafing)) / (Bd4 (leafing) + Bd3 (leafing)) (3)

  In Formula (3), NDVI (leafing time) is the planting life degree (NDVI) of the leafing time, Bd3 (leafing) is the reflectance in the visible light region (Band3), and Bd4 (leafing) is the leafing time. The reflectance in the near-infrared light region (Band 4) at the time of leafing is shown. When the two images are compared, the difference in the measured vegetation such as the loss of leaves such as deciduous trees due to the difference in the seasons is detected and the difference in the vegetation viability (NDVI) is detected. Indicated.

  FIG. 11 is a diagram two-dimensionally showing a difference normalized vegetation index (ΔNDVI) calculated by calculating a difference between normalized vegetation index (NDVI) values in different seasons. The calculation is obtained from the following equation (4).

ΔNDVI = NDVI (leafing time) −NDVI (falling leaf time) (4)

  In Formula (4), “NDVI (leafing time)” indicates an NDVI value in a season with a leaf of a broadleaf tree, and “NDVI (falling time)” indicates an NDVI value in a season without a leaf of a broadleaf tree. As shown in this figure, basic data was generated to identify land use categories that include vegetation status.

  FIG. 12 is a diagram two-dimensionally showing the result of performing land use classification determination processing based on the values of NDVI and ΔNDVI for each point. In the land use classification determination process, the values of NDVI and ΔNDVI are determined based on a predetermined threshold. The land use classifications shown in this figure show the results of classification into "regular forest", "deciduous forest", "grassland", "urban area", and "field / development area".

Fig. 13 shows the results of land use classification ("regular forest", "deciduous forest", "grassland", "urban area", "field and development area") classified based on the value of ΔNDVI for each point. Set the annual evapotranspiration corresponding to each usage category. An example of the set value of annual evapotranspiration for land use classification is shown. “Regular forest” and “deciduous forest” shall be 700.08 mm. The “grassland” is 630.72 mm. The “city area” is 422.64 mm. The “field / development area” shall be 700.08 mm. It is the figure which showed two-dimensionally the result classified into the shade display according to the result of the set annual evapotranspiration. It is shown that the thinner the color shown in the figure, the higher the annual evapotranspiration.
As described above, the evapotranspiration calculating unit 31 sets the annual evapotranspiration for each region as the possible evapotranspiration based on the information from the satellite image data obtained by remote sensing.

Next, the amount of rainfall recharge at each point will be described.
The rainfall recharge amount indicates the amount of the rainfall at that point that penetrates the ground and is recharged as groundwater. As mentioned above, it was shown that the amount of evapotranspiration at each point varies with changes in the situation such as vegetation at each point. Before infiltration and recharge to groundwater, the amount of evaporation from the ground surface or divergence due to vegetation is corrected by the following equation (5) to determine the amount of rainfall recharge.

(Rain recharge) = (rainfall-possible evapotranspiration) / 2 (5)

In Equation (5), the right side is divided by 2 because it is set and approximated as a proportionality constant for determining the amount that flows out as surface water and does not permeate that point.
As described above, the rainfall recharge amount calculation unit 32 performs the calculation process represented by the above equation (5) based on the rainfall amount information and the annual evapotranspiration amount at each point.

With reference to the figure, the setting of the reference point of the groundwater pressure on the reference surface of the surface water where the groundwater appears on the ground surface will be described.
When the ground surface becomes lower than the groundwater surface, the groundwater is saturated and appears on the surface. In other words, the groundwater surface on the ground that touches the water level of the river matches.
FIG. 14 is a diagram for explaining a reference surface (pressure head 0 m) for calculating the groundwater surface.
This figure (a) is sectional drawing which showed the cross section of the direction which crosses a river. As shown in this figure, the water brought by the rain penetrates and becomes groundwater. Water in the state where the gap included in the geology is filled with water is called groundwater. The state filled with groundwater is called saturated state. Where saturated geology touches the surface, groundwater appears as surface water. This surface water becomes a river that flows on the surface. Based on the position of the water surface of this river, the water pressure due to the groundwater at each point at the reference height is called the pressure head. The pressure head is an index indicating the difference between the height of this standard and the groundwater surface. The water pressure due to the difference in altitude of the reference plane from the altitude of 0 m is referred to as the position head. The sum of pressure head and position head is called total head. The total head is an index indicating the pressure difference of the groundwater at that point, and the groundwater moves due to the pressure difference.
The total head value is shown as equation (6).

(Total head) = (Position head) + (Pressure head) (6)

This figure (b) is a figure which shows the processing result in the pressure head 0m setting part 33 which specified the water surface which has appeared on the ground surface in the object area. In this figure, meshes are two-dimensionally constructed in the horizontal direction, and the points indicated by the intersections of the meshes indicate the places such as rivers that appear as surface water with white circles (◯).
The pressure head 0 m setting unit 33 can identify a point covered with surface water from remote sensing data at the time of leaf fall. The satellite image data used for the determination of surface water uses information indicating the difference in reflectance in the near-infrared region (Band 4) at the time of leaf fall. Since near infrared rays are absorbed on the surface of the surface water, the reflectance is shown as a low value, so that the position covered with the surface water can be specified from a location showing a value equal to or lower than the threshold value. The pressure head 0 m setting unit 33 superimposes information on the result determined to be covered with surface water on the map information, and sets the point of the pressure head 0 m with the position of the water surface such as a river or a lake as a reference plane. Set. The point of the pressure head 0 m is a reference point indicating the groundwater level 0 m indicating the height of the surrounding groundwater surface.

The calculation process of the total head distribution will be described with reference to the drawing.
FIG. 15 is a bird's eye view showing the result of setting the geological information for the position and depth of each point in the symmetric range. The ground surface and the edge of the symmetry range are shown in cross section. The shading shown in this figure shows different geology. In accordance with the geological information constituting the area, the geology constituting each point is set based on the position and depth. The geological distribution map shown in this figure is created from the set information. In association with the geological characteristics shown in this distribution map, the hydraulic conductivity and unsaturated characteristics of the position and depth of each point are set. The total head calculation processing unit 34 calculates the total head value based on the above-described rainfall recharge amount, pressure head 0 m distribution, topographic altitude data, hydraulic conductivity of each position / depth, and information on unsaturated characteristics.

The calculation process of the total head distribution will be described with reference to the drawing.
FIG. 16 is a diagram illustrating an example of the total water head distribution obtained by the arithmetic processing. The curve shown in this figure is a curve in which points indicating the same total pressure head are connected. The undulations of the groundwater surface can be calculated from this total head distribution.
Moreover, FIG. 17 is a figure which shows the actual measurement data of the groundwater surface elevation observed in the area | region shown in FIG. FIG. 16 and FIG. 17 are compared, and it can be seen that the shape of the curve of the head distribution shown in FIG. 16 and the shape of the curve showing the head distribution obtained from the actual measurement data of FIG. 17 show the same tendency. That is, the water head distribution obtained from the calculation result processed based on the rainfall recharge corrected based on the remote sensing image data was verified by actual measurement data.

The groundwater transfer route and transfer time calculation processing will be described with reference to the drawings.
Based on the total head distribution information obtained by the total head calculation processing unit 34, the topographic elevation data, the hydraulic conductivity of the position / depth of each point, the information on the unsaturated characteristics and the effective porosity, the groundwater transfer route and the transfer time are determined. calculate.
Groundwater shifts due to the difference in total head value between adjacent points. In other words, the groundwater flows in a direction perpendicular to the curve indicated by the total head distribution shown in the above head distribution map. In the portion where the change of the head value indicated by the head value distribution curve is large, that is, in the portion where the head value distribution curve is densely shown, the flow velocity of the groundwater is increased. On the other hand, in the portion where the change of the head value is gentle, that is, the portion where the head value distribution curve is shown sparsely, the flow rate of the groundwater becomes small.

Calculate the groundwater flow direction and flow velocity at each location and depth at each location. First, reference points arranged in a grid are set at points referred to by the position and depth of each point. At the position of the reference points arranged in a grid, a minute cube having a length of one side between the reference points is defined, and the amount of water flowing in and out from each surface of the cube is calculated. The calculated amount of water flowing in and out is decomposed into components in the three-dimensional coordinate axis direction. By using the value decomposed into the components in the coordinate axis direction, the transition of water at the reference point can be indicated by a vector.
FIG. 18 is a diagram illustrating the flow of groundwater.
The mesh shown in this figure shows a lattice indicating the position, and shows a three-dimensional model of the ground in consideration of the altitude of each point. Moreover, the arrow shown by this figure shows the transfer direction of the groundwater at the point. At points where the directions indicated by these arrows are aligned and indicate the same direction, this indicates that groundwater flows in that direction. The length of the arrow line indicates the amount of groundwater transferred, that is, the flow velocity.

The groundwater transfer route calculation process will be described with reference to the figure.
FIG. 19 is a diagram illustrating a transfer route of groundwater. Selection of the groundwater transfer route is calculated by connecting the direction of groundwater transfer at each point of the route.
For the calculation of the migration path, two calculation methods can be selected. The first calculation method is a method of designating a recharge location and calculating a flow direction starting from the recharge location. The second calculation method is a method of designating a predetermined depth at a position where groundwater reaches and calculating a route that can reach the position. In this method, the route is selected retroactively with respect to the actual direction of groundwater flow.
The first calculation method is a method of selecting a route along the direction in which the actual groundwater flows. From the point selected as the start point, select a reference point that is in the direction to which the vector indicating the destination of the groundwater at that point refers, and select the reference point that is in the direction to which the vector of the reference point refers It can be calculated by repeating the process.
In the second calculation method, the first reference point that makes the closest reference to the vector of each reference point is selected from the reference points around the arrival point of the groundwater. Similarly, from the reference points around the first reference point, the reference point that makes the closest reference to the vector of each reference point is selected as the second reference point. This process is repeated, and the place where the ground surface is reached becomes the groundwater recharge point.
In the present embodiment, description will be made using the second calculation method.

A method for calculating the transition time required when the groundwater moves along the groundwater transition path determined by the above processing will be described.
For the calculation of the groundwater transfer time, flow velocity (Darcy flow velocity) calculation using Darcy's law is known. In the calculation of the transition time by Darcy flow velocity, the transition time (path distance / Darcy flow velocity) is calculated under the condition that the effective porosity is assumed to be 100% (percent), and the effective porosity (%) is set. The transition time can be obtained by the correction process. The relationship is shown in Equation (7).

(Transition time by actual flow rate)
= (Path distance) / (Dalcy flow velocity) x (effective porosity) (7)

As shown by the equation (7), the Darcy flow velocity value with an effective porosity of 100% is generally slower than the actual flow velocity value. The migration rate will be determined by the amount of groundwater injected.
For example, if the transition time obtained by the Darcy flow velocity is calculated as 700 years and the effective porosity of the path is 7%, the transition time by the actual flow velocity is obtained as 49 years.
As described above, the groundwater transfer route / transfer time calculation processing unit 35 can specify the transfer route of the groundwater and obtain the transfer time.

  Subsequently, each processing procedure performed in groundwater origin analysis and information used for the processing will be described. Information used for each process of groundwater origin analysis in the groundwater origin analysis system 100 is stored in various databases allocated to the storage unit 70, and in accordance with instructions such as recording / reference from each functional unit that performs each process. The control storage processing unit 50 performs recording / reading processing to various databases allocated to the storage unit 70. In the following description of the processing, processing such as recording / reference that each functional unit instructs the control storage processing unit 50, recording / reading processing of the storage unit 70 performed by the control storage processing unit 50, and each processing performed by the control storage processing unit 50 The notification process to the function unit will be described as being included in the process in which each function unit performs a recording / reading process to various databases. The results calculated and calculated by each functional unit are displayed on the display unit 90 via the output processing unit 80. For display on the display unit 90, the output processing unit 80 refers to information recorded in each storage unit according to an instruction from the control storage processing unit 50 to the output processing unit 80, and generates an output screen based on the information. It is displayed on the display unit 90.

FIG. 20 is a flowchart showing groundwater origin analysis processing.
The groundwater origin analysis process in the groundwater origin analysis system 100 includes a plurality of processes shown in the figure.
First, the ion concentration water quality information determination processing unit 10 in the groundwater origin analysis system 100 performs a determination process of the similarity of the groundwater origin from the degree of coincidence of the ratios of the ion concentrations of river water and groundwater and the degree of coincidence of the water quality (step SA10). ). Subsequently, the isotope ratio determination processing unit 20 in the groundwater origin analysis system 100 performs a recharge height determination process from the degree of coincidence of the isotope ratios of river water and groundwater (step SB20). Subsequently, the groundwater transfer calculation processing unit 30 in the groundwater origin analysis system 100 performs the groundwater transfer calculation processing according to the following procedure. First, the evapotranspiration calculating unit 31 performs a calculation process for obtaining an evapotranspiration amount for each point from satellite image data captured by the artificial satellite, and calculates a possible evapotranspiration amount for each point (step SC31). The rainfall recharge calculating unit 32 performs a calculation process based on the information on the possible evapotranspiration at each point and the rainfall at each point, and calculates the rain recharge at each point (step SC32). The pressure head 0 m setting unit 33 performs calculation processing based on the position, latitude, longitude, and altitude information of the river indicated in the satellite image data, and the point where the pressure head indicates 0 m, that is, the groundwater becomes surface water as a river. The point appearing is set (step SC33). The total head calculation processing unit 34 performs calculation processing to obtain the total head from the rainfall recharge amount and the pressure head distribution at each point, the topographic elevation data, and the permeability coefficient and saturation characteristics at each point and depth. Information is calculated (step SC34). The groundwater transfer route / transition time calculation processing unit 35 performs a calculation process for obtaining the groundwater transfer route and the transfer time from the total head distribution at each point and the hydraulic conductivity, saturation characteristics, and effective porosity for each point / depth, The groundwater transfer route and the transfer time are calculated (step SC35).

Details of the processing of each step described above will be described in order.
FIG. 21 is a diagram showing a data structure of data used for ion concentration analysis processing and water quality information processing.
The ion concentration information database shown in FIG. (A) includes “latitude (X)”, “longitude (Y)”, “depth”, “sulfate ion”, “bicarbonate ion”, “chlorine ion”, “calcium ( “Ca) ions”, “magnesium (Mg) ions”, “sodium (Na) ions / potassium (K) ions”. This figure shows an example in which an ion concentration information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate the sampling location of the collected water. “Depth” indicates the depth of collection at the collection point. Each item of “sulfate ion”, “bicarbonate ion”, “chlorine ion”, “calcium (Ca) ion”, “magnesium (Mg) ion”, “sodium (Na) ion / potassium (K) ion” The concentrations of (SO ₄ ²⁻ ) ion, (HCO ₃ ⁻ ) ion, (Cl ⁻ ) ion, (Ca ²⁺ ) ion, (Mg ²⁺ ) ion, (Na ⁺ ) ion and (K ⁺ ) ion are shown. For each piece of information registered based on the water information collected as a sample and the water information of various points that have already been measured, data in units of rows is constructed, and “latitude (X)”, “ “Longitude (Y)” and “depth” are referred to as keys.

  Further, the water quality information database shown in FIG. 5B has items including “latitude (X)”, “longitude (Y)”, “depth”, “electric conductivity”, and “water temperature”. This figure is an example in which the water quality information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate the sampling location of the collected water. “Depth” indicates the depth of collection at the collection point. “Electrical conductivity” indicates the electrical conductivity of the collected water. “Water temperature” indicates the water temperature when the collected water is collected. For each piece of information registered based on the water information collected as a sample and the water information of various points that have already been measured, data in units of rows is constructed, and “latitude (X)”, “ “Longitude (Y)” and “depth” are referred to as keys.

Next, with reference to a figure, the process of the various processes of the groundwater origin analysis system 100 is demonstrated. In the process description below,
FIG. 22 is a flowchart showing ion concentration analysis processing.
The input processing unit 40 receives the ion / water quality information data input from the ion / water quality information system (ion / water quality information data 210), and uses the river water measurement data as the key to the ion concentration information database. Register (step Sa1). Further, the input processing unit 40 performs an input process of the ion concentration / water quality information of the groundwater to be determined and registers it in the water quality information database (step Sa2). The ion concentration water quality information determination processing unit 10 analyzes the tendency of the ion concentration based on the registration data of each point registered in the ion concentration information database. The ion concentration water quality information determination processing unit 10 arranges main ions in an array, arranges each point at a position indicating the ion concentration value, and connects the points to the hexadiagram (FIG. 2). Browse). Further, the ion concentration water quality information determination processing unit 10 performs principal component analysis processing, determines the similarity of the registration data at each point, and records the determination result in the storage unit (step Sa3). The ion concentration water quality information determination processing unit 10 refers to the data registered in the water quality information database, and performs linear regression analysis on the altitude based on an index indicating each water quality (see FIG. 3). Similar trends are shown for groundwater from the same water source. It is determined that the similarity is high when the distance to the obtained straight line is included in a predetermined determination range (step Sa4).

  The ion concentration water quality information determination processing unit 10 analyzes the similarity of the groundwater origin. In this analysis, determination is made from both results of similarity determination by ion concentration analysis at each point and trend analysis of similarity determination information using water quality information (step Sa5). The ion concentration water quality information determination processing unit 10 determines that the similarity of the groundwater origin is high when the determination shows that both the ion concentration tendency and the water quality tendency are similar, and records the determination result in the storage unit. The determination process is terminated (step Sa6). The ion concentration water quality information determination processing unit 10 determines that the similarity of the groundwater origin is low when both the ion concentration tendency and the water quality tendency are not similar, records the determination result in the storage unit, and performs the determination process. The process ends (step Sa7). The ion concentration water quality information determination processing unit 10 determines that the similarity determination result is ambiguous when the similarity is observed in either the ion concentration trend or the water quality trend and no similarity is found in the other, and the determination result is unclear. Is stored in the storage unit and the determination process is terminated (step Sa8).

FIG. 23 is a diagram showing a data structure of data used for stable isotope ratio analysis processing.
The stable isotope ratio information database shown in the figure has items including “latitude (X)”, “longitude (Y)”, “depth”, “oxygen isotope ratio”, and “recharge altitude”. This figure is an example in which a stable isotope ratio information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate the sampling location of the collected water. “Depth” indicates the depth of collection at the collection point. “Oxygen isotope ratio” indicates the isotope ratio of oxygen ( ¹⁸ O), which is a stable isotope of collected water. The “recharge altitude” indicates the recharge altitude calculated by stable isotope ratio analysis processing from the oxygen ( ¹⁸ O) isotope ratio of the collected water. For each piece of information registered based on the water information collected as a sample and the water information of various points that have already been measured, data in units of rows is constructed, and “latitude (X)”, “ “Longitude (Y)” and “depth” are referred to as keys.

FIG. 24 is a flowchart showing a stable isotope ratio analysis process.
The input processing unit 40 receives isotope information data input from the isotope information system (isotope information data 220), and uses stable isotope ratio information such as river water as the key to information on the measurement point. Record in the information database (step Sb1). The isotope ratio determination processing unit 20 analyzes the tendency of the stable isotope ratio with respect to the altitude (see FIG. 5) based on the information stored in the stable isotope ratio information database such as river water (step Sb2). The input processing unit 40 receives the isotope information data input from the isotope information system (isotope information data 220), and uses the stable isotope ratio information database with the stable isotope ratio information of the groundwater as the information on the measurement point. (Step Sb3).
The isotope ratio determination processing unit 20 analyzes the tendency by performing linear regression analysis from the relationship of the weight of the stable isotope ratio with respect to the elevation of the measurement point (see FIG. 7). The isotope ratio determination processing unit 20 determines the water system according to the result of the linear regression analysis (see FIG. 8) in which the information on the target groundwater is analyzed for each water system (step Sb4).
The isotope ratio determination processing unit 20 calculates the recharge height based on the stable isotope ratio data of groundwater (see FIG. 7), and records the calculation result in the stable isotope ratio information database (step Sb5).

FIG. 25 is a diagram illustrating a data structure of data used for the evapotranspiration calculation process.
The evapotranspiration calculation processing database shown in FIG. (A) includes “latitude (X)”, “longitude (Y)”, “falling time Bd3”, “falling time Bd4”, “leafing time Bd3”, “arrival”. It has items consisting of “leaf time Bd4”, “falling time NDVI”, “leafing time NDVI”, “ΔNDVI”, “land use classification”, and “possible evapotranspiration”. This figure is an example in which the evapotranspiration calculation processing information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate the latitude and longitude of information constituting the satellite image. “Falling time Bd3” and “Falling time Bd4” are reflectances (advanced) provided by satellite images taken in the visible light region (Band3 region) and the near-infrared region (Band4 region), respectively. ). The “leafing time Bd3” and “leafing time Bd4” are reflections of the ground surface provided by satellite images taken in the visible light region (Band3 region) and the near-infrared region (Band4 region), respectively, at the time of leafing. Indicates the rate (adved). “Falling time NDVI” and “Leaving time NDVI” indicate the degree of vegetation life at the falling time and the falling time, respectively. “ΔNDVI” indicates a result of subtracting “leafing time NDVI” from “leaved leaf time NDVI”. “Land use classification” indicates an index of land use forms classified based on the value of (ΔNDVI). “Possible evapotranspiration” indicates a possible evapotranspiration according to the selected (land use classification). For each point in the range provided by the satellite image, data in units of rows is constructed and referred to using “latitude (X)” and “longitude (Y)” as keys.

Also, the reference threshold value database shown in FIG. 5B shows certain items from “a”, “b”, “c”, “d”, “e”, “f”, and “g”. This figure is an example in which the reference threshold value database is two-dimensionally arranged.
“A” refers to an NDVI value at the time of leaf setting and indicates a threshold value for determining the normal leaf area and the urban area. A point exceeding the threshold “a” is determined to be an normal leaf area. “B” and “c” indicate thresholds for distinguishing between urban areas and field areas from among the urban areas determined by the threshold value “a” with reference to ΔNDVI of the point. A point where ΔNDVI exceeds “b” and does not satisfy “c” is defined as an urban area. “D” indicates a threshold value for distinguishing an evergreen forest and a deciduous region from among vegetation areas determined by the threshold value “a” with reference to ΔNDVI at that point. “E” indicates a threshold for distinguishing deciduous forest and grassland from the deciduous area determined by the threshold “d” with reference to ΔNDVI at that point. “F” indicates a threshold value for determining a water area by referring to the reflectance (adved) “deciduous leaf time Bd4” of the ground surface provided by satellite image data taken in the near infrared region (Band4 region) during the leaf fall time. . “G” is a threshold value for determining a snow covered area with reference to the reflectance (advedo) “deciduous time Bd4” of the ground surface provided by satellite image data taken in the near-infrared region (Band4 region) during the leaf fall time Indicates.

FIG. 26 is a flowchart showing evapotranspiration calculation processing.
The input processing unit 40 receives the satellite image data measured from the visible light region and the near infrared region input from the remote sensing system 231 and receives the received satellite image data in the evapotranspiration calculation processing database. "latitude (X)", and records the information "longitude (Y)" as a key (step _Sc 31 1). The evapotranspiration calculating unit 31 refers to each of the adobe “leaved leaf time Bd3”, “leaved leaf time Bd4”, “leaved leaf time Bd3”, and “leaved leaf time Bd4” stored in the evapotranspiration amount calculation processing database. arithmetic processing of vegetation index NDVI performed (see FIGS. 9 and 10), and records the evapotranspiration processing database (step _Sc 31 2). The evapotranspiration calculating unit 31 refers to the normalized vegetation indices “deciduous leaf time NDVI” and “leafing time NDVI” stored in the evapotranspiration amount calculation processing database, and calculates the difference normalized vegetation index ΔNDVI (FIG. 11). You can refer to), and records the evapotranspiration processing database (step _Sc 31 3). The evapotranspiration calculating unit 31 sets thresholds “a”, “b”, “c”, “d”, “e”, “f”, and “g” in the reference threshold database. Each threshold value is set to a value that enables separation by referring to two different satellite image data and data indicated by the difference normalized vegetation index ΔNDVI. (Step _Sc 31 4)

The evapotranspiration calculating part 31 determines whether it is a vegetation area. The determination is based on whether or not the “leafing time NDVI” stored in the evapotranspiration calculation processing database exceeds the threshold “a” stored in the reference threshold database (Step S1). Sc ₃₁ 5). As a result of the vegetation area determination, if it is determined that the area is not a vegetation area (No), the evapotranspiration calculating unit 31 determines whether or not the point is an urban area. The determination is based on whether or not “ΔNDVI” stored in the evapotranspiration calculation processing database exceeds the threshold “b” stored in the reference threshold database and is less than “c”. It is carried out (step _Sc 31 6). When it is determined that the condition is satisfied (Yes) as a result of the urban area determination, the evapotranspiration calculating unit 31 determines that the amount of change in ΔNDVI is “urban area”, and an index indicating the urban area is calculated. It is recorded in the "land use classification" of the database (step _Sc 31 7). When it is determined that the condition is not satisfied (No) as a result of the urban area determination, the evapotranspiration calculating unit 31 determines that the field is a “field” having a large amount of change in ΔNDVI, and calculates an evapotranspiration amount index indicating the field. It is recorded in the "land use classification" of the processing database (step _Sc 31 8).

As a result of the vegetation area determination, if it is determined that the area is a vegetation area (Yes), the evapotranspiration calculating unit 31 determines whether or not the point is the normal leaf area. The determination is based on whether or not “ΔNDVI” stored in the evapotranspiration calculation processing database is less than the threshold “d” stored in the reference threshold database (step Sc _31). 9). As a result of the determination of the normal leaf area, if it is determined that the area is the normal leaf area (Yes), the evapotranspiration calculation unit 31 determines that it is an “every-leaf forest” that does not change according to the season, and uses an index indicating the normal leaf forest. Recorded in the “land use classification” of the evapotranspiration calculation processing database (step Sc ₃₁ 10).

As a result of the normal leaf area determination, when it is determined that the area is not the normal leaf area (No), the evapotranspiration calculating unit 31 determines that the point has a seasonal change, and determines whether or not it is a deciduous forest area. I do. The determination is based on whether or not “ΔNDVI” stored in the evapotranspiration calculation processing database is less than the threshold “e” stored in the reference threshold database (step Sc _31). 11). As a result of the determination of the deciduous forest area, when it is determined that the area is a deciduous forest area (Yes), the evapotranspiration calculation unit 31 determines that the deciduous forest has a small change in ΔNDVI and indicates the deciduous forest. The index is recorded in the “land use classification” of the evapotranspiration calculation processing database (step Sc ₃₁ 12). As a result of the determination of the deciduous forest area, when it is determined that the area is not a deciduous forest area (No), the evapotranspiration calculating unit 31 determines that the change in ΔNDVI is “grassland” and evaporates an index indicating the grassland. Recorded in the “land use classification” in the sprinkling calculation processing database (step Sc ₃₁ 13).

The evapotranspiration calculating unit 31 refers to the “land use classification” index (see FIG. 12) stored in the evapotranspiration calculation processing database, and converts it into a conversion constant set in advance according to the index. Then, the calculation (see FIG. 13) for obtaining the possible evapotranspiration for each land use category is performed, and the obtained possible evapotranspiration is recorded in the “possible evapotranspiration” in the evapotranspiration calculation processing database (step Sc _31). 14).

FIG. 27 is a diagram illustrating a data structure of data used for the rainfall recharge amount calculation processing.
The rainfall recharge information database shown in the figure has items including “latitude (X)”, “longitude (Y)”, “rainfall”, and “rainage recharge”. This figure is an example in which a rainfall recharge information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate locations where there is rainfall. “Rainfall” indicates the rainfall at that point. “Rain recharge” indicates the recharge of water that permeates into the groundwater. In the rainfall recharge information database, data in units of rows is configured for each point, and is referred to using “latitude (X)” and “longitude (Y)” as keys.

FIG. 28 is a flowchart showing the rainfall recharge amount calculation processing.
The input processing unit 40 receives the rainfall data input from the rainfall information system 232 and records the received rainfall data in the rainfall recharge information database (step Sc ₃₂ 1).
The rainfall recharge amount calculation unit 32 refers to the evapotranspiration amount calculation processing database and acquires the “possible evapotranspiration amount” at each point (step Sc ₃₂ 2).
Rainfall recharge amount calculation unit 32 calculates the rainfall recharge amount for each land area, and be recorded in the "rainfall recharge amount" of rainfall recharge amount information database (step Sc 32 _3).

FIG. 29 is a diagram illustrating a data structure of data used for the pressure head 0 m setting process.
The topographic elevation information database shown in FIG. 1A has items including “latitude (X)”, “longitude (Y)”, and “altitude”. This figure is an example in which the terrain elevation information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate the location of the point indicating the altitude. “Altitude” indicates the altitude of the point. In the terrain elevation information database, data in units of rows is configured for each point, and is referred to using “latitude (X)” and “longitude (Y)” as keys.

  The pressure head 0 m setting calculation information database shown in FIG. 5B has items including “latitude (X)”, “longitude (Y)”, “groundwater surface coordinate value”, and “pressure head 0 m”. This figure is an example in which the pressure head 0 m setting calculation information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate a place where the pressure head 0 m is obtained. The “groundwater surface coordinate value” is an index indicating the position of the water surface of the groundwater. That is, the value indicated by the vertical coordinate is shown. “Pressure head 0 m” indicates the water surface of groundwater, and is “1” when it corresponds to, for example, a river. Note that the initial value of “pressure head 0 m” is set to “0” indicating a region other than the water area. In the pressure head 0 m setting calculation database, data in units of rows is configured for each point, and is referred to using “latitude (X)” and “longitude (Y)” as keys.

FIG. 30 is a flowchart showing a pressure head 0 m setting process.
Input processing unit 40 receives the terrain elevation data inputted from the map information system 233 records the terrain elevation data received in the terrain elevation information database (step Sc 33 _1). The pressure head 0 m setting unit 33 refers to the evapotranspiration calculation processing database, and acquires reflectance (albedo) data “falling time Bd4” of the near-infrared region Band4 at the falling time of each point. Further, the pressure head 0 m setting unit 33 refers to the reference threshold value database and acquires threshold value information “f” (step Sc ₃₃ 2). The pressure head 0m setting unit 33 determines whether or not each point is a water area covered with surface water. When it is determined that the point is a water area, the pressure head 0m setting calculation information database stores “pressure head 0m”. "1" is recorded. The determination refers to “deciduous leaf timing Bd4” stored in the evapotranspiration calculation processing database, and determines whether or not the threshold “f” stored in the reference threshold database is exceeded (determination condition) Step Sc ₃₃ 3). When the pressure head 0m setting unit 33 determines that it is a water area as a result of the determination as to whether or not it is a water area, it records “1” in “pressure head 0 m” of the pressure head 0 m setting calculation information database (FIG. 14). (Refer to (b)) (Step Sc ₃₃ 4).

FIG. 31 is a diagram illustrating a data structure of data used for the total head value calculation process.
The geological information database shown in FIG. 1A has items including “geology (material)”, “water permeability coefficient X”, “water permeability coefficient Y”, “water permeability coefficient Z”, and “effective porosity”. This figure is an example in which the geological information database is represented in a two-dimensional array. “Geology (material)” indicates a material constituting the geology of the point. “Water permeability coefficient X”, “water permeability coefficient Y”, and “water permeability coefficient Z” are the water permeability coefficients in the directions indicated by the three-dimensional coordinates. Here, the Z direction indicates the vertical direction. “Effective porosity” indicates the proportion of space contained per unit deposition. The geological information database includes data in units of rows for each geology, and is referred to using “geology (material)” as a key.

  The total head value calculation information database shown in FIG. 2B has items including “latitude (X)”, “longitude (Y)”, “depth”, “geology”, and “total head value”. This figure shows an example in which the total head value calculation information database is two-dimensionally arranged. “Latitude (X)” and “Longitude (Y)” indicate points where the total head value is calculated. “Depth” indicates the depth of a point indicated by “latitude (X)” and “longitude (Y)”. “Geology” indicates an index indicating the geology of a point indicated by “latitude (X)”, “longitude (Y)”, and “depth”. The “total head value” indicates a total pressure head (see FIG. 14 (a)) indicating the sum of the position head of the altitude indicated by the pressure head 0 m and the pressure head calculated based on the altitude of the pressure head 0 m. The total pressure head is an indicator of the groundwater level. In the total head value calculation database, data in units of rows is configured for each point, and is referred to using “latitude (X)”, “longitude (Y)”, and “depth” as keys.

FIG. 32 is a flowchart showing the total head value calculation process.
Total head processing section 34 refers to the terrain elevation database, acquires can refer to terrain elevation data (step Sc 34 _1). The total head calculation processing unit 34 refers to the pressure head 0 m setting calculation information database, refers to the coordinates of the pressure head 0 m, acquires information, and authorizes the water area (step Sc ₃₄₂ ). Input processing section 40, the geological information database, and registers the permeability and unsaturated penetration characteristics (step Sc 34 _3). The total head calculation processing unit 34 calculates the amount of groundwater in and out at each point and depth. The total head processing section 34 performs a calculation of total head value for each point are recorded in the "total head value" of total head value calculation information database (step Sc 34 _4). Total head processing section 34 performs conversion processing to the total water head value distribution information from the "total head value" in each point (see FIG. 16) (step Sc 34 _5).

FIG. 33 is a diagram illustrating a data structure of data used for the groundwater transfer route / time calculation process.
The point geological information database shown in FIG. (A) includes “latitude (X)”, “longitude (Y)”, “depth”, “permeability coefficient X”, “permeability coefficient Y”, “permeability coefficient Z”, “ It has an item consisting of “effective porosity”. This figure is an example in which the geological information database is represented in a two-dimensional array. “Latitude (X)” and “Longitude (Y)” indicate points where the total head value is calculated. “Depth” indicates the depth of a point indicated by “latitude (X)” and “longitude (Y)”. “Water permeability coefficient X”, “water permeability coefficient Y”, and “water permeability coefficient Z” are the water permeability coefficients in the directions indicated by the three-dimensional coordinates. Here, the Z direction indicates the vertical direction. “Effective porosity” indicates the proportion of space contained per unit deposition. The geological information database includes data in units of rows for each geology, and is referred to using “latitude (X)”, “longitude (Y)”, and “depth” as keys.

  The groundwater transfer route / time calculation processing database shown in FIG. (B) includes “No.”, “Latitude (X)”, “Longitude (Y)”, “Depth”, “Transition speed X”, “Transition speed Y”. ”,“ Transition speed Z ”, and“ Altitude ”. This figure is an example in which the groundwater transfer route / time calculation information database is two-dimensionally arranged. “No.” indicates a transfer order. “Latitude (X)”, “Longitude (Y)”, and “Depth” indicate the position of a reference point that identifies the transition path. “Transition speed X”, “Transition speed Y”, and “Transition speed Z” indicate the transition speed of groundwater in each coordinate axis direction at the reference point. “Altitude” indicates the altitude of the ground surface at the latitude and longitude indicating the reference point. That is, the altitude when the “depth” becomes 0 m indicates the recharge height.

FIG. 34 is a flowchart illustrating the groundwater transfer route / time calculation process.
The input processing unit 40 records the effective porosity in the geological information database (Step Sc ₃₅ 1). Groundwater migration path-shift time calculation processing unit 35 refers to the total head value operation information database to obtain information "Geology", "total head value" (step Sc 35 _2). The groundwater transfer route / transfer time calculation processing unit 35 refers to the geological information database of each point from the information on the “geology” of the place indicated by “latitude (X)”, “longitude (Y)”, and “depth”. Information of “water permeability coefficient X”, “water permeability coefficient Y”, and “water permeability coefficient Z” according to (material) is recorded. Moreover, underground water migration path-shift time calculation processing unit 35 refers to the geological information database, acquires the "effective porosity" is recorded in each point geological information database (step Sc 35 _3). The groundwater transfer route / transfer time calculation processing unit 35 calculates the amount of transfer of groundwater at each point and depth (see FIG. 18). The groundwater transfer route / transfer time calculation processing unit 35 identifies the transfer route of groundwater at each point and depth (see FIG. 19). Moreover, underground water migration path-shift time calculation processing unit 35 will compute a transition time based on Darcy flow velocity based on the movement path specified (Step Sc 35 ₄₎

The groundwater transfer route / transfer time calculation processing unit 35 refers to the determination result in step SA1, and the ion concentration information of the point recorded as an area along the route from the recharge height indicated by the transfer route determined above. acquires quality information (step _Sc 35 5). The groundwater transfer route / transfer time calculation processing unit 35 refers to the determination result in step SB1 and acquires the stable isotope information of the point recorded as the recharge height area determined above (step Sc ₃₅ 6). . The groundwater transfer route / transition time calculation processing unit 35 obtains the groundwater transfer route / transition time calculation processing unit 35 by processing when it is determined that the similarity of the groundwater origin is high as a result of the determination of the ion concentration information / water quality information. It is determined that the relevance of the given migration path is high. As a result of the determination of the ion concentration information and the water quality information, when it is determined that the similarity of the origin of the groundwater is low, it is determined that the validity of the transfer route obtained by the processing of the groundwater transfer route / transfer time calculation processing unit 35 is low. . As a result of the determination of the ion concentration information and the water quality information, when it is determined that the similarity of the groundwater origin is unclear, there is some influence on the validity of the transfer route obtained by the processing of the groundwater transfer route / transfer time calculation processing unit 35. It is determined that it is difficult to determine from the obtained transition path, and the determination result is recorded in the storage unit. Also, the recharge height indicated by the stable isotope information is compared with the height of the recharge point on the determined transition route. As a result of comparison, if the value is within the predetermined range, it is determined that the similarity is high from both results, and if the value is outside the predetermined value range, the determination result is determined that the similarity is low from both results the records in the storage unit (step _Sc 35 7).
Thus, the reliability of the determination process result is determined by determining based on a plurality of determination process results.

  The above groundwater origin analysis system 100 has a computer system inside. The above-described process of calculating the groundwater origin is stored in a computer-readable recording medium in the form of a program, and the above-described process is performed by the computer reading and executing this program. Here, the computer-readable recording medium means a magnetic disk, a magneto-optical disk, a CD-ROM, a DVD-ROM, a semiconductor memory, or the like. Further, the computer program may be distributed to the computer via a communication line, and the computer that receives the distribution may execute the program.

The groundwater origin analysis system 100 sets an osmotic water amount, which is difficult to measure directly, based on satellite image data of the vegetation area. Deviation can be reduced. In addition, information on a wide area is obtained by using satellite image data. And the groundwater origin analysis system 100 can improve the accuracy of the model calculated | required by approximation by performing the correction | amendment according to the condition for every point, and performs the calculation process of an accurate groundwater transfer route and transfer time. Is possible.
The groundwater origin analysis system 100 also verifies the validity of the recharge point indicated by the calculation result of the calculation process of the groundwater transfer route and the transfer time by associating and verifying the results of the determination process by a plurality of determination methods. The reliability of the obtained result can be confirmed. As a plurality of determination methods, ion concentration ratio analysis, water quality information analysis, stable isotope ratio analysis, groundwater transfer route and transfer time analysis, and the like can be used.

The present invention is not limited to the above embodiments, and can be modified without departing from the spirit of the present invention. In the calculation of groundwater recharge altitude using stable isotopes in the groundwater origin analysis system 100 of the present invention, oxygen ¹⁸ O is exemplified as a stable isotope, but calculation is performed using deuterium ² H (D). It is also possible to perform processing.
Moreover, although electrical conductivity and water temperature were illustrated about the determination by water quality, it is also possible to utilize acidity (pH (pea etch)).
Moreover, the groundwater origin analysis system 100 of the present invention may execute various processes using a plurality of computers in addition to executing various processes by one computer, and the division of processes into each computer is arbitrary. It is. At that time, information is moved between storage units of each computer by performing communication processing using a communication line or moving through a readable recording medium.

  The step of specifying the groundwater origin from the degree of coincidence of the ion concentration ratios according to the present invention corresponds to the processing of step SA10 performed by the ion concentration water quality information determination processing unit 10. Further, the step of specifying the dependent altitude from the degree of coincidence of the isotope ratios according to the present invention corresponds to the processing of step SB20 performed by the isotope ratio determination processing unit 20. Further, the step of calculating the evapotranspiration amount for each region from the satellite image data of the vegetation area according to the present invention corresponds to the process of step SC31 performed by the evapotranspiration amount calculation unit 31. Further, the step of calculating the amount of seepage water from the evapotranspiration amount and the precipitation value stored in the storage unit according to the present invention corresponds to the process of step SC32 performed by the rainfall recharge amount calculation unit 32. The step of setting the position of the groundwater level 0 m for each region from the satellite image data indicating the river region stored in the storage unit according to the present invention corresponds to the process of step SC33 performed by the pressure head 0 m setting unit 33. Further, the step of calculating the regional head value from the amount of infiltrated water and the altitude information at each point according to the present invention corresponds to the processing of step SC34 performed by the total head calculation processing unit 34. Further, the step of calculating the groundwater transfer route from the distribution of the head value according to the present invention corresponds to the process of step SC35 performed by the groundwater transfer route / transfer time calculation processing unit 35.

  Moreover, in other embodiment of this invention, the groundwater origin analysis system which calculates a rainfall recharge amount correctly based on quantitative data is provided. As shown in FIG. 69, precipitation (precipitation amount P) in a certain target area is evapotranspiration (evapotranspiration E) that evaporates into the atmosphere in the area, and rain recharge (rainfall) that penetrates underground in the area. Recharge amount I) and outflow from the basin to the outside of the basin (outflow amount R). That is, the rainfall recharge amount I is obtained by (precipitation amount P−evapotranspiration amount E−runoff amount R). In the groundwater origin analysis, since the rainfall recharge I is an input for groundwater simulation, it is important to accurately calculate each of the precipitation P, the evapotranspiration E, and the runoff R. The evapotranspiration amount E can be accurately calculated based on the satellite image data as described above. Therefore, in another embodiment of the present invention, runoff analysis and precipitation analysis are performed to calculate runoff R and precipitation P, and precisely calculate rainfall recharge I according to the above-described relationship.

In conventional runoff analysis, it has been common to use river flow data at a flow monitoring station closest to the target area. That is, the runoff rate (annual river flow ÷ dividual precipitation) is calculated from the river flow data, and this is multiplied by the precipitation in the target area to calculate the runoff in the target area.
Other runoff analysis in the past includes analysis using runoff rates determined for each terrain and geology, and analysis relying on qualitative evaluation using topographic elements.

  However, in the conventional runoff analysis, there is no runoff rate to be used in the target area where there is no flow monitoring station. Even if there is a difference in topographical features in the target area, there is no choice but to use a uniform outflow rate. In other words, in the conventional runoff analysis, it was not possible to perform an analysis reflecting the nature of the topography, such as water flowing easily if the topography is steep and difficult to flow if the topography is slow.

Therefore, in the groundwater origin analysis system of the present invention, in the runoff analysis, paying attention to the topography most closely related to the surface water runoff, the runoff index calculated from topographic measurement and statistical analysis, and the existing runoff The data is compared, the presence or absence of a correlation between the two is determined, and a correlation equation (regression equation) is calculated. Then, the outflow data of an unknown target area where no outflow data exists is calculated using the outflow index and the regression equation.
Thereby, in the outflow amount analysis, there is an effect that the outflow amount in the unknown target region can be estimated.
In addition, in the runoff analysis, the runoff index is calculated based on the data obtained from the topographical measurement instead of the uniform runoff calculation in the conventional runoff analysis. There is an effect that the amount can be calculated.
Furthermore, in the groundwater origin analysis system of the present invention, it is possible to accurately calculate the rainfall recharge amount based on the quantitative data (evapotranspiration, runoff amount and precipitation amount) as described above.

Below, the groundwater origin analysis system by one Embodiment of this invention is demonstrated with reference to drawings.
FIG. 35 is a block diagram showing the groundwater origin analysis system 100a according to this embodiment.
In FIG. 35, the same components as those in FIG. 1 that are not in FIG. 35 have the same functions as those in FIG.
In FIG. 35, a newly added information input system 200a is shown.
The information input system 200a includes an elevation value information system (DEM data 241) that provides an elevation value in a calculation target area, a river flow information system (river flow data 242) that provides an outflow amount in the calculation target area, A weather information system (weather data 243) that provides data such as rainfall, wind speed, temperature and sunshine in the target area is provided.

  The groundwater transfer calculation processing unit 30a performs arithmetic processing based on various information input from the information input system 200a, paying attention to the topography most closely related to surface water outflow, and is calculated from topography measurement and statistic analysis. Compare and examine the runoff index and existing runoff data, and estimate the runoff in the unknown target area.

  The groundwater transfer calculation processing unit 30a is recharged as groundwater at a point where it has rained, and calculates the transition route and transition time until it reaches as the groundwater of the dredging by the topography and altitude difference of the path through which the groundwater flows and the environment. This is a determination processing unit. The groundwater transfer calculation processing unit 30a includes an evapotranspiration calculation unit 31, a rainfall recharge calculation unit 32a, a pressure head 0m setting unit 33, a total head calculation processing unit 34, a groundwater transfer route / transition time calculation processing unit 35, and an outflow calculation. A unit 36 and a precipitation calculation unit 37 are provided. The rainfall recharge amount calculation unit 32 a is based on the information of the evapotranspiration amount calculated by the evapotranspiration amount calculation unit 31, the outflow amount calculated by the outflow amount calculation unit 36, and the precipitation amount calculated by the precipitation amount calculation unit 37. To calculate the rainfall recharge. Further, the pressure head 0m setting unit 33 performs calculation processing based on image data (not shown in FIG. 35) taken from an artificial satellite and information on latitude / longitude and altitude, and a point where the pressure head shows 0 m, That is, a point where groundwater appears as surface water as a river is set. The total head calculation processing unit 34 calculates the total head value information by calculating based on the information on the point where the rain recharge amount and the pressure head at each point show 0 m, the latitude longitude and the altitude information. The groundwater transfer route / transfer time calculation processing unit 35 performs calculation processing based on the total head value information of each point to calculate the groundwater transfer route and the transfer time.

The outflow amount calculation unit 36 includes a topography measurement unit 361, a statistical processing unit 362, an outflow index determination unit 363, and an outflow amount estimation unit 364. The terrain measurement unit 361 performs basin division on the calculation target region based on DEM data (terrain data) input from the elevation value information system (DEM data 241), calculates basin division data, and also divides the basin. Calculate topographical measurement data at. The statistical processing unit 362 performs factor analysis based on the calculated topographic measurement data, and extracts a component (factor) having a correlation with the ease of water flow. In addition, the outflow index determination unit 363 calculates an outflow index based on the extracted component (factor). The outflow amount estimation unit 364 performs a comparison determination between the calculated outflow index and the river flow data (the outflow amount of the target basin) input from the river flow information system (river flow data 242). Calculate the specific flow rate.
The precipitation calculation unit 37 calculates the precipitation according to the altitude value of the DEM data based on the weather data input from the weather information system (weather data 243).

  The input processing unit 40a receives information from the connected information input system 200 and the information input system 200a. The input processing unit 40a is connected to each storage unit allocated to the storage unit 70a (not shown in FIG. 35, but corresponds to the storage unit 70 in FIG. 1). , Corresponding to the control storage processing unit 50 in FIG. 1) is recorded. As information input from the information input system 200 and the information input system 200a, either information recorded on a computer-readable medium or information input by communication processing performed via a communication line can be selected. . The input processing unit 40a includes an input unit such as a mouse and a keyboard, performs processing for detecting information input from the input unit, and inputs the detected result to the control storage processing unit 50a.

Next, functions of various processes of the outflow amount calculation unit 36 will be described with reference to the drawings. The terrain measurement unit 361 in the outflow amount calculation unit 36 performs basin division of the calculation target region based on DEM data input from the elevation value information system (DEM data 241), calculates basin division data, and is divided. The topographic measurement data in the basin is calculated. The DEM data refers to a digital elevation model (Digital Elevation Model), which is raster data (lattice data) in which elevation values are stored in each grid. The DEM data is not only used for displaying the terrain but also used for various measurements and analyzes such as calculating the inclination from the altitude. For example, the well-known numerical map of the Geographical Survey Institute uses 50-meter mesh grid DEM data. The landform measurement unit 361 divides the target area for each basin based on the DEM data in which the elevation value is stored in each grid. The boundary of the divided watershed is a boundary corresponding to one watershed or a boundary composed of a plurality of watersheds. That is, in each divided basin, the rain that falls within the basin flows into the river closest to the main stream. In the following description, a basin and a grid are distinguished from each other, and each basin is described as being configured by a grid. For example, the precipitation in the basin is assumed to be a value obtained by integrating the precipitation for each grid over all the grids in the basin.
FIG. 36 is a diagram two-dimensionally showing the result of the division processing performed by the landform measurement unit 361. From this figure, it can be seen that the target area is divided into basins along a boundary corresponding to one watershed or a boundary composed of a plurality of watersheds. In addition, the divided basins are a total of 69 basins including 9 basins (see FIG. 47) in which river flow measurement described later is performed and 60 basins in which measurement is not performed. The landform measurement unit 361 can perform the watershed division process shown in FIG. 36 based on the gradient (inclination amount) calculated from the elevation value of the DEM data.

The topographic measurement unit 361 performs topographic measurement for each divided basin. Topographic measurement items are slope (inclination), Laplacian (slope curvature), Laplacian SD (standard deviation), basin volume, basin undulation number (stiffness index), basin average erosion height, channel generation, basin exit And the coefficient (distortion degree, kurtosis), the basin shape ratio, the channel shape ratio, the branching ratio (R _1/2 , R _2/3 ), the channel frequency, the channel gradient skewness, The basin area.
Here, Laplacian is a differential of the gradient, that is, a secondary differential of the altitude, and represents the unevenness of the terrain, and Laplacian SD represents the complexity of the terrain. The basin average erosion height represents the difference between the current elevation and the ridge surface (topography before erosion). The basin undulation number is an index representing the steepness of the average topography in the basin, and is defined as a value obtained by dividing the basin volume by the basin area by the power of 1.5. Further, the basin average erosion height is obtained by summing up the erosion for each grid in the DEM data within the target basin and dividing by the basin area. The skewness is an index that represents a symmetric shift in the frequency distribution of the distance from the basin exit to the upstream area, and the kurtosis is an index that represents the extent of the bottom of the distribution. The basin shape ratio is an index indicating whether the planar shape of the basin is round or elongated, and is defined by a value obtained by squaring the basin maximum side length and dividing by the basin area. Even if the shape of the basin is circular, if the length of the main channel is longer than the maximum basin length (width of the basin), it must be treated as having the same basin structure as that of the elongated basin. Is difficult to distinguish. Therefore, in order to evaluate the shape of the basin with respect to the length of the main channel (maximum channel length), the channel shape ratio is calculated. This is defined as a value obtained by squaring the maximum flow path length in the basin and dividing by the basin area. The larger the value of the channel shape ratio, the longer the shape becomes vertically elongated (the shape is long and narrow in the direction along the river main stream), and can be used as an index indicating the topography where water hardly flows. Even if the shape of the basin is a circular basin, the maximum channel length becomes long when the main channel is developed along the circumference of the circle. For this reason, the flow channel shape ratio of the basin may be the same as the flow channel shape ratio of the elongated basin. The branching ratio indicates the ratio of the number of channels in the order in a certain basin, and the branching ratio of the primary flow (number of channels N1) and the secondary (number of channels N2) into which the primary channel flows is R _{1. / 2} = N1 / N2. Further, the branching ratio of the tertiary flow path (flow path number N3) into which the secondary flow path flows is obtained by R _2/3 = N2 / N3. The flow channel frequency is an index indicating how many flow channels are present per unit area. The basin gradient skewness is an index representing the relationship between the average gradients obtained by calculating the average gradient with respect to a certain point from the measurement point to the upstream at all points upstream.

  The statistic processing unit 362 in the outflow amount calculation unit 36 performs multivariate analysis (factor analysis) to reduce the terrain measurement result measured by the terrain measurement unit 361, and is common to the terrain measurement items (analysis variables). Calculate fewer factors than analysis variables. That is, in this embodiment, the statistic processing unit 362 extracts a plurality of components (factors) having a correlation with the ease of water flow.

In performing the factor extraction, the statistic processing unit 362 performs the following calculation processes (1) to (9). (1) For each analysis variable, calculate the average value and standard deviation of the terrain measurement results in the whole basin. (2) The measurement result in each basin is standardized for each analysis variable, and a standardized matrix Z is calculated. Standardization is obtained by (measurement result−average value) / standard deviation. (3) A correlation matrix R between analysis variables is calculated. (4) The square of the correlation coefficient of the multiple regression analysis obtained by using the SMC (Squared Multiple Correlation) method and using the diagonal elements of the correlation matrix R as the dependent variables and the other variables as independent variables (decision variable) To obtain a new matrix R ^′ . (5) The eigenvalue and factor loading for each factor are calculated from the new matrix R ^′ by the Jacobian method. (6) It is determined whether to use up to the first factor among all the factors depending on whether the eigenvalue exceeds a preset threshold value. For example, a factor having an eigenvalue of 1 or more is selected. (7) In order to facilitate the interpretation of factors, the coordinate load (varimax rotation) of the factor loading selected in (6) is performed, and the factor loading (factor loading matrix A) and contribution for each factor after the rotation. Calculate the rate. (8) Factor score of each basin is calculated by standardized data matrix × inverse matrix of correlation matrix R × factor load matrix A. (9) The factor loading (factor loading matrix A) is determined based on a preset threshold for each factor.

FIG. 37 shows the eigenvalue, contribution rate, and cumulative contribution rate calculated by the statistic processing unit 362. The numbers 1 to 11 in the vertical direction indicate factor numbers, and are arranged so that the eigenvalues are changed from a larger value to a smaller value from the smaller number to the larger number. The eigenvalue is an index that indicates how much information (variance) of the entire data obtained by topographic measurement is explained by each factor. When all the eigenvalues in the initial sum of squares of load are integrated, it is the same as the number of factors. 11 Further, the contribution rate is an index indicating what percentage of the total information amount can be explained by each factor, and this figure shows that 30.261% can be explained only by the first factor. The cumulative contribution rate is an index indicating what percentage of the total information amount can be explained up to the nth factor. Note that the varimax rotation is performed to eliminate the difficulty of interpreting the latent factors, so the cumulative contribution rate up to the fourth factor does not change before and after the rotation.
FIG. 38 shows factor load amounts (factor load matrix A) of factors 1 to 4 calculated by the statistic processing unit 362 in the above-described calculation process (8). The items shown in the vertical direction in the figure are analysis variables in the terrain measurement. The horizontal numbers 1 to 4 indicate factor numbers, and the values indicate factor loadings. Factor loading is a correlation coefficient that indicates the strength of the relationship between the factor and the analysis variable, and an analysis variable that has a positive factor loading has a positive correlation with the factor and a negative value. The analysis variable is negatively correlated with the factor.

39 to 42 show factor loadings corresponding to factors 1 to 4, with eleven analysis variables when measuring topography in the vertical direction, and the horizontal direction corresponding to the analysis variables of factors 1 to 4. Indicates the factor loading. In each figure, it can be said that an analysis variable having a larger factor load has a higher degree of explanation of the factor. In FIG. 39, the factor loading of factor 1 is as large as 0.904 for the basin average erosion height, 0.899 for the terrain complexity (Laplacian SD), and 0.592 for the basin undulations among the analysis variables. 1 and positive correlation. These analysis variables are all analysis variables related to the fineness of the terrain and the undulations of the terrain. Therefore, the factor 1 is determined as a factor indicating the undulations. In FIG. 40, the factor load amount of factor 2 is as large as 0.739 for the flow channel shape ratio and 0.731 for the branching ratio R _1/2 , and factor 2 is determined to be a factor indicating the shape of the basin and flow channel. Is done. In FIG. 41, the factor load amount of factor 3 is as follows: the distance from the basin outlet and the coefficient (distortion) relating to the shape are as large as 0.841, the basin shape ratio is 0.786, and factor 3 is a factor indicating the basin shape. To be judged. Further, in FIG. 42, the factor load amount of factor 4 has a flow channel frequency as high as 0.736, and factor 4 is determined as a factor indicating the density of the channel.
The statistic processing unit 362 in the outflow amount calculation unit 36 determines a plurality of components (factors 1 to 4) having such a correlation with the ease of water flow for each factor based on a preset threshold value. .

  The outflow index determination unit 363 in the outflow amount calculation unit 36 selects a plurality of factors from the component having the larger eigenvalue from the plurality of components (factors) having correlation with the ease of water flow extracted by the statistic processing unit 362. . For example, the outflow index determination unit 363 selects the above-described factor 1 and factor 2. As described in detail below, factor 1 (hereinafter referred to as factor number PC1) is a factor directly related to the ease of water flow, and factor 2 (hereinafter referred to as factor number PC2) is a flow of water. It is a factor that is directly related to bitterness.

FIG. 43 is a two-dimensional diagram in which the factor score of factor 1 (factor number PC1) for each divided area is divided into five levels and each basin is displayed in shades. The deeper the color area, that is, the basin where the factor score is larger, the ridge develops, that is, the basin where the valley is deep and the undulation is steep. On the other hand, a light-colored area, that is, a basin with a small factor score, has no ridge development and can be said to be a gentle basin. The ease of water flow is understood as mass transfer and its speed, but the direction of movement of the substance (water) and its speed are proportional to the gradient of the topography. This is because the gradient is a factor that determines the horizontal component of gravity. Terrain where slopes with steep slopes are gathered is generally expressed by the word steep, and on the contrary, terrain where slopes with gentle slopes are gathered, such as plains and the earth, is expressed as gentle.
That is, the basin having a large factor score of factor 1 is a steep basin with a sharp undulation, and is a basin where water easily flows. On the other hand, a basin with a small factor score of factor 1 is a gentle basin with few undulations and is a basin where water does not flow easily.

FIG. 44 is a two-dimensional diagram in which the factor score of factor 2 (factor number PC2) for each divided region is divided into five levels and each basin is displayed in shades. The deeper the color area, that is, the larger the basin factor, the basin shape becomes a vertically elongated basin shape (long and narrow in the direction along the river main stream). Conversely, the smaller the factor score, the closer the basin shape is to a circular or horizontally elongated basin shape (a shape that is short and wide in the direction along the river main stream).
Even if the shape of the basin is approximate, the factor score is different if the shape of the flow path is different. FIG. 45 is an explanatory diagram schematically showing this state. In the figure, the basin shape is represented by a circle or an ellipse, and the vertical or horizontal straight lines indicate the main stream length of the river in the basin. The part where the main stream length of the river is in contact with the river basin is the outlet of the flow path, and a low-order river flows into the main stream length. In the figure, as it goes to the right, the shape of the basin becomes circular or elongated horizontally. As the shape becomes circular or laterally elongated, the distance to the outlet of the flow path becomes shorter, and water becomes easier to flow. However, as shown in the figure, even with the same elongated shape, the shape of the basin that is elongated along the river main stream (the basin shape on the left in the figure) and the shape of the basin that is elongated in the direction perpendicular to the river main stream (the basin shape on the right in the figure) So the distance to the basin exit is different. That is, when the basin shape is an elongated basin shape along the river main stream as in the basin shape on the left side of the figure, the distance to the basin outlet becomes long, so that it becomes difficult for water to flow.
In other words, a basin with a large factor score of factor 2 is a basin shape that is vertically elongated (long and narrow basin shape along the river main stream), and a river basin with a long main stream length. Indicates a watershed that is difficult to flow. On the other hand, in a basin where the factor score of factor 2 is small, the shape of the basin is a circular or horizontally elongated basin (a shape that is short and wide in the direction along the river main stream), and the river main stream length is short. Yes, that is, a watershed where water can flow easily.

The outflow index determination unit 363 calculates an outflow index for each basin using the factor score calculated for each area. Specifically, the outflow index determination unit 363 classifies the factor scores into five groups by Jenks' natural classification method (optimal classification method). Here, it may be possible to calculate the outflow index using the factor score as it is, but instead of returning the reduced topographic measurement data to data with variations again, the index is calculated in groups. To do.
There are other classification methods for grouping, such as equal interval classification, equality classification, interval definition classification, and standard deviation classification. The natural classification method is adopted. This is because terrain measurement data in the natural world is unlikely to have a uniform distribution like a normal distribution, and often has a variation distribution reflecting the features of the terrain. The outflow index determination unit 363 calculates division points according to a preset division number, and divides the factor score distribution into a plurality of groups, for example, five groups. Then, for each factor (factor number PCi), 5 points, 4 points,..., 1 point and a score R _PCi are _assigned in order from a group with a large factor score to a small group.

The outflow index determination unit 363 calculates an outflow index for each basin using the following equation.
Outflow index = (Granted R _PC1 ) × W _PC1 + (6- (Granted R _PC2 )) × W _PC2
Here, W _PC1 and W _PC2 are expressed by the following equations.
W _PC1 = C _PC1 / (C _PC1 + C _PC2 )
W _PC2 = C _PC2 / (C _PC1 + C _PC2 )
C _PCi is the contribution ratio of the factor (factor number PCi) calculated by the statistic processing unit 362. That is, since the contribution rate of each factor is different, W _PC1 and W _PC2 are used as weighting variables reflecting the difference in contribution rate in the outflow index calculation formula.

  FIG. 46 is a two-dimensional view in which the outflow index for each divided basin is classified into five levels and the basin is displayed in shades. This figure shows the factor score of factor 1 (factor number PC1) directly related to the ease of water flow and the factor 2 (factor number PC2) directly related to the difficulty of water flow It is shown that it was classified by the outflow index reflecting the score.

The outflow amount estimation unit 364 in the outflow amount calculation unit 36 obtains a correlation between the outflow index of a part of the basin calculated by the outflow index determination unit 363 and the actual outflow amount, and when there is a positive correlation, Calculate regression equation between runoff index and runoff.
There are two types of actual runoff: observed values accumulated at runoff stations over several decades and actually measured values measured at the exits of some basins.
In order to obtain the actual measurement value, the river flow rate (equal to the outflow amount of the basin) was measured at the exit of some basins among the basins where the outflow index was calculated. However, when comparing with the flow rate index, the river flow rate differs depending on the size of the basin area, so we decided to compare it with the index normalized by the basin area called specific flow rate. The specific flow rate can be obtained by specific flow rate = river flow rate / basin area. The unit of the specific flow rate is m ³ / (second · 100 km ² ).

FIG. 47 is a two-dimensional view in which the specific flow rate actual measurement values of the nine basins in which the river flow rate is measured are classified into five levels, and the basins are displayed in shades.
FIG. 48 is a scatter diagram in which the outflow index (x) and the specific flow rate (y) of the basin where the specific flow rate is measured in FIG. 47 is plotted, and the straight line in the drawing represents a regression line. The regression line is represented by y = 0.5258x−0.7027. In the figure, R ² is a value R ² obtained by squaring Pearson's product-moment correlation coefficient R. From the value R ² = 0.6954, there is a strong correlation between the outflow index and the specific flow rate. I understand.
FIG. 49 uses the regression line obtained above to convert the calculated outflow index for each region into a specific flow rate for each region, and shows the basin where the topographic measurement was performed according to the converted specific flow rate result. It is a two-dimensional diagram displayed in shades. As a result, it was proved that the specific flow rate of the unknown 60 basins, that is, the outflow amount, can be calculated from the relationship between the outflow index and the specific flow rate in the nine basins.

  Note that, as described above, the actual measurement value for obtaining the correlation with the outflow index includes the observation value. The observed value is the annual river flow (average value from several years to several decades) at several discharge stations. In addition, when estimating the correlation between the observed value and the runoff index, the annual river flow is estimated using the value (runoff rate) obtained by dividing the annual river flow by the annual precipitation in the basin where the flow monitoring station exists. Annual precipitation can be obtained from the annual rainfall map by integrating the catchment area including the flow monitoring station.

Next, estimation of precipitation will be described with reference to the drawings.
The precipitation calculation unit 37 in the groundwater transfer calculation processing unit 30a performs spatial interpolation based on the result of correcting the precipitation data, and calculates precipitation for each basin. Spatial interpolation refers to estimating precipitation in the entire target area based on precipitation data from several weather stations in the target area when estimating the spatial distribution of precipitation in the target area. A spline method is known as a spatial interpolation method. However, in order to perform spatial interpolation, it is necessary to perform the following processes (1) and (2). (1) It is necessary to perform processing that takes into account errors in precipitation data. For example, in the observation with precipitation gauges in northern Japan and the Honshu Sea of Japan, the biggest error factor is the capture loss that snow and rain do not enter the precipitation gauge due to the wind. Snow is particularly susceptible to wind, so the capture loss ratio is large. Therefore, it is necessary to correct the supplemental loss. (2) It is necessary to perform processing that reflects the “elevation dependency” of rainfall. Generally, the higher the altitude, the higher the amount of precipitation. However, since the weather station is located in a relatively low place (altitudes from a few meters to several hundreds of meters), it is necessary to use the precipitation data from the weather station. Interpolation does not reflect elevation dependence at high altitudes. Therefore, it is necessary to perform processing reflecting altitude dependency.

  The precipitation calculation unit 37 considers the supplemental loss of the precipitation data of the observed value, and calculates the corrected precipitation P based on the observed value p by the equation P = p × (1 + mU). Here, U represents the wind speed at the opening of the precipitation meter at the observatory, and the unit is m / second. Further, m is a coefficient determined by the precipitation meter and the solid / liquid of precipitation, and the unit is second / m. For example, in the case of a formula in which the type of precipitation meter falls, the coefficient m is 0.213 for snow and 0.0454 for rain.

The precipitation calculation unit 37 determines whether there is a correlation with the altitude based on the corrected precipitation P. If there is a correlation, the precipitation calculation unit 37 further corrects the corrected precipitation P to reflect the altitude dependency. . FIG. 50 is a graph showing the relationship between the annual precipitation (after correction for supplementary loss) and the altitude at a weather station. The straight line in the figure represents a regression line. The regression line is represented by y = 0.40989x + 523.94. In the figure, R ² is a value R ² obtained by squaring Pearson's product moment correlation coefficient R. From the value R ² = 0.8914, there is a strong correlation between altitude and annual precipitation. I understand.
The precipitation calculation unit 37 uses the rate of change a (unit: mm / 1m) obtained from the regression formula (general formula y = ax + b) to correct the annual precipitation at the weather station to a value b at an altitude of 0 m. Perform spatial interpolation.
That is, it is converted into precipitation data (grid) that does not depend on elevation once, and the precipitation of the entire target area is estimated by spatial interpolation. Thereafter, the precipitation calculation unit 37 adds a value corresponding to the elevation value of the DEM data to the precipitation after spatial interpolation based on the increase / decrease rate a. For example, based on the rate of increase / decrease, if the grid is located at an altitude of 500 m, 0.4989 (value of a) × 500 = 250 mm is added to the value obtained by spatial interpolation.
FIG. 51 is a two-dimensional diagram in which the corrected rainfall considering the altitude dependence is displayed in shades in the basin, and shows that the darker the point, the more the corrected rainfall is. From FIG. 51, it can be seen that the estimated precipitation amount (lattice) reflecting the topographical difference (altitude difference) in the basin was calculated.

Then, the process procedure performed by rainfall recharge calculation and the information used for the process are demonstrated. FIG. 52 is a flowchart showing processing performed in rainfall recharge calculation. The rainfall recharge amount calculation process includes a plurality of processes shown in FIG.
First, the terrain measurement unit 361 in the outflow amount calculation unit 36 performs basin division and terrain measurement processing in the divided basin (step SD10). Subsequently, the statistic processing unit 362 in the outflow amount calculation unit 36 performs statistic processing for calculating a factor score for each basin based on the measured topographic data (step SD11). Subsequently, the outflow index determination unit 363 in the outflow amount calculation unit 36 performs an outflow index examination process for calculating an outflow index based on the calculated factor score in each basin (step SD12). The outflow amount estimation unit 364 in the outflow amount calculation unit 36 determines whether or not there is a correlation between both based on the calculated outflow index and information on the outflow amount (river flow rate) of a part of the basin. When it determines, the outflow amount estimation process which calculates the estimated outflow amount of all the basins is performed (step SD13). Next, the precipitation calculation part 37 performs the precipitation estimation process which calculates the estimated precipitation in each basin based on precipitation (observed value) (step SD14). The rainfall recharge calculating unit 32a performs a rain recharge calculating process for calculating the rainfall recharge in each basin and each grid based on the outflow, precipitation, and evapotranspiration estimated in each basin (step SD15). .

Hereinafter, details of the processing in each of the above steps will be described in the order of runoff, precipitation, and evapotranspiration calculation. First, the terrain measurement process performed by the terrain measurement unit 361 will be described.
FIG. 53 is a diagram showing a data structure of data used for the terrain measurement process. The terrain database shown in FIG. 1A has items including latitude “X”, longitude “Y”, and altitude “H” based on grid DEM data. This figure is a two-dimensional representation of the terrain database. The terrain database is composed of data in units of rows, and the altitude “H” is referred to using latitude “X” and longitude “Y” as keys. Further, the basin division database shown in FIG. 5B has items including “basin number”, latitude “X”, longitude “Y”, and altitude “H”. This figure is a two-dimensional representation of the terrain division database. The topographic division database is composed of data in units of rows, and latitude “X”, longitude “Y”, and altitude “H” are referred to with “basin number” as a key.
The topographic measurement database shown in Fig. (C) includes "basin No", "gradient", "Laplacian", "Laplacian SD", "basin volume", "basin undulation number", "basin average erosion height", " Road generation ”,“ kurtosis ”, which is a coefficient related to the distance from the basin outlet and its shape, and“ distortion ”,“ basin shape ratio ”,“ flow basin shape ratio ”which are coefficients related to the distance from the basin outlet and its shape. ”, Branching ratio“ R1 / 2 ”, branching ratio“ R2 / 3 ”,“ flow path frequency ”,“ distortion degree of flow path gradient ”, and“ basin area ”. This figure is a two-dimensional representation of the topographic measurement database. The topographic measurement database is composed of data in units of rows for each basin, and each data is referred to using the basin No as a key.

Next, the terrain measurement process will be described with reference to the drawings.
FIG. 54 is a flowchart showing the terrain measurement process.
The input processing unit 40a receives the DEM data input from the elevation value information system (DEM data 241), and converts the received DEM data 241 corresponding to the measurement target area into “X”, “Y”, and “ H ”(step Sd ₁₀ 1). Next, the terrain measurement unit 361 divides the measurement target area into k basins based on “X”, “Y”, and “H” registered in the terrain database, and displays “basin no. allocate "," X "in the basin split database records with the" Y "and" H "(step _Sd 10 2). Next, the terrain measurement unit 361 refers to “X”, “Y”, and “H” of the basin division database for each basin No, performs the ground measurement for each analysis variable, and displays the measurement result as “basin No”. and as a key measurement item (analyzing variable), and records the Morphometry database (step _Sd 10 3).

Next, statistical processing performed by the statistical amount processing unit 362 will be described.
FIG. 55 is a diagram showing a data structure of data used for statistical processing. The statistical analysis constant database shown in FIG. 1A has items consisting of “n”, “m”, “th1”, and “th2”. This figure is a two-dimensional representation of the statistical analysis constant database. n indicates the number of analysis variables when performing factor analysis, and m indicates the number of factors when performing varimax rotation. In addition, th1 indicates a threshold for determining the number of factors m in varimax rotation, and th2 indicates a threshold for performing factor interpretation (selection of analysis variable) based on the factor loading (factor loading matrix A). . The factor load database shown in FIG. (B) has items consisting of “analysis variable j” and factor numbers “PC1” to “PCm”. The factor loading database forms a matrix of n rows and m columns, and factor loadings are recorded in the matrix components. For example, a _nm represents the factor loading of the mth factor (PCm) nth analysis variable. Further, the contribution rate database shown in FIG. 3C has items consisting of “C _PC1 ” to “C _PCm ”, and the contribution rates of the factor numbers PC1 to PCm are registered and referred to.

  FIG. 56 shows the data structure of data used for statistical processing. The factor score database shown in FIG. 1A has items including “basin number” and factor numbers “PC1” to “PCm”. The factor score database records each factor score for each k-divided basin. Further, the interpretation result database shown in FIG. 5B has items including “basin number” and factor numbers “PC1” to “PCm”. In the interpretation result database, the determination result for each basin divided into k is recorded. The determination result indicates a determination result when it is determined whether or not the factor load amount shown in FIG. 55 (b) is equal to or greater than a threshold th2. If the determination result is greater than or equal to th2, the determination result is 1; 0 is recorded for each basin and for each factor number.

Next, statistical processing will be described with reference to the drawings.
FIG. 57 is a flowchart showing statistical processing. The statistical processing unit 362 refers to “n” of the statistical analysis constant database, and sets the measurement item (analysis variable) of the topographic measurement database to n according to the set numerical value n using the basin No (1 to k) as a key. (Step Sd ₁₁ 1). Next, the statistical processing unit 362 performs principal component analysis (factor analysis) using n × k pieces of data, calculates a new matrix R ^′, and calculates eigenvalues for each factor from the new matrix R ^′ by the Jacobian method. calculate. The statistical processing unit 362 refers to “th1” of the statistical analysis constant database, selects a factor having an eigenvalue equal to or greater than the threshold, using the set numerical value as a threshold, and sets the number of selected factors in the statistical analysis constant database. Record in m. Also, factor numbers PC1, PC2,..., PCm are assigned in order of the selected eigenvalues.

The statistical processing unit 362 calculates a factor load matrix after varimax rotation for m factors, and records “analysis variable j” and “factor numbers PC1 to PCm” in the factor load amount database as keys. Further, the statistical processing unit 362 calculates the contribution rate of each factor and records it in “C _PC1 ” to “C _PCm ” of the contribution rate database. Statistical processing unit 362 calculates the factor score of each basin, the factor scores database records "basin No", factor number "PC1" - the "PCm" as a key (Step _Sd 11 2). Next, the statistical processing unit 362 refers to the threshold value set in th2 of the statistical analysis constant database, and the statistical processing unit 362 interprets the principal component (factor interpretation) based on the factor load. Specifically, referring to the factor load recorded in the factor load database, 1 is determined to be a value equal to or greater than the threshold, and 0 is determined to be a value less than the threshold. the records "basin No", factor number "PC1" - the "PCm" as a key (step _Sd 11 3).

Next, the outflow index calculation process performed by the outflow index determination unit 363 will be described.
FIG. 58 is a diagram showing a data structure of data used in the outflow index calculation process. The outflow index constant database shown in FIG. 1A has items consisting of “p” and “q”. “P” indicates the number of factors selected, and “q” indicates the number of steps to classify the factor score. The classification threshold database shown in FIG. 2B has items including “threshold No” and factor numbers “PC1” to “PCp”. In the classification threshold database, thresholds for classifying factor scores into q levels are recorded by the number of selected factors p multiplied by (q-1). For example, when the selection number p of the factor number is 2 and the factor score is classified into q = 5 stages, 8 threshold values are recorded. Further, weighting database shown in FIG. (C) _has an entry consisting of _{W PC1 ~W PCp, W PC1 ~W} PCp is recorded on the basis of the contributions of factors PC1～PCp. For example, when the number of selected factors is 2, W _PC1 = C _PC1 / (C _PC1 + C _PC2 ) and W _PC2 = C _PC2 / (C _PC1 + C _PC2 ) are calculated and recorded as described above.

  FIG. 59 is a diagram showing a data structure of data used in the outflow index calculation process. The score database shown in FIG. 1A has items including “classification No” and factor numbers “PC1” to “PCp”. In the score database, “acquired scores” for each classification number corresponding to factors PC1 to PCp are set and registered in advance. For example, when the selection number p of the factor number is 2 and the factor score is classified into q = 5 levels, natural numbers of 1 to 5 are registered for each factor from the smaller classification No. The ranking database shown in FIG. (B) has items including “basin number” and factor numbers “PC1” to “PCp”. In the ranking database, “scores” for each basin are recorded corresponding to the factor numbers PC1 to PCp. That is, the data recorded in the “acquired score” of the score database is recorded using “basin No” and factor numbers “PC1” to “PCp” of the ranking database as keys. Further, the outflow index database shown in FIG. 3C has items including “basin number” and “outflow index”. In the runoff index database, runoff indices are recorded for each basin.

Next, the outflow index calculation process will be described with reference to the drawings.
FIG. 60 is a flowchart showing the outflow index calculation processing. The outflow index determination unit 363 refers to “p” in the outflow index constant database, and selects a principal component (selects a factor) according to a set numerical value. For example, when the numerical value is 2, factor 1 and factor 2 are selected (step Sd ₁₂ 1). Next, the outflow index determination unit 363, the principal component scores of the factor scores database (factor scores), refers to the "basin No" and factor number "PC1" - "PCp" as a key (Step _Sd 12 2). The outflow index determination unit 363 refers to “q” in the outflow index constant database, and uses the Jenks natural classification method (optimal classification method) as the classification threshold of the referenced factor score according to the set numerical value. Thus, (q−1) division points where the data change amount is large are calculated. Then, the calculated division points are recorded as a classification threshold value in the classification threshold value database, and “threshold No.” and factor numbers “PC1” to “PCp” are recorded as keys for each factor in order from the smallest threshold value. For example, in the example shown in FIGS. 43 and 44, for the factor number PC1, four values of the classification thresholds −1.45272, −0.33224, 0.15012, and 0.81666 are set to the factor number PC2. , Four values of classification thresholds -1.20055, -0.39586, 0.25619, and 1.45265 are calculated and recorded in the classification threshold database in order of increasing value from threshold No1 for each factor. To do. Also, the outflow index determination unit 363 refers to the threshold value recorded in the classification threshold value database using “threshold No.” and factor numbers “PC1” to “PCp” as keys, and which threshold No. indicates the factor score in each basin. It is determined whether to enter the group, and the classification number is determined. For example, if the factor score is less than the threshold No 1 threshold, the classification No is 1; if the factor score is between the threshold No 1 threshold and the No 2 threshold, the classification No is 2. Next, the outflow index determination unit 363 refers to the score database using “classification No” and factor numbers “PC1” to “PCp” as keys, and refers the acquired score to the ranking database as “basin number” and factor number. “PC1” to “PCp” are recorded as keys (step Sd ₁₂ 3). Next, the outflow index determination unit 363 refers to “C _PC1 ” to “C _PCp ” of the contribution rate database, and calculates weighting variables “W _PC1 ” to “W _PCp ” based on the contribution rates of the factors. Record each factor in the weighting database. The outflow index determination unit 363 refers to the ranking database “basin No” and the factor numbers “PC1” to “PCp” as keys, calculates the outflow index for each basin based on the weighting variables W _{PC1 to} W _PCp , to the outflow index database records "basin No" as a key (step _Sd 12 4).

Next, the outflow amount estimation process performed by the outflow amount estimation unit 364 will be described.
FIG. 61 is a diagram illustrating a data structure of data used in the outflow amount estimation process. The river flow measurement database shown in FIG. 1A includes items including “basin number”, “river flow measurement data”, and “specific flow”. In the river flow measurement database, the river flow measurement data of the basin where the data exists and the specific flow of the basin are registered. The flow rate threshold value database in FIG. 5B has an item consisting of “S1”. In S1, a threshold for determining whether there is a correlation between the specific flow rate and the outflow index is set. Further, the specific flow rate database shown in FIG. 3C includes items including “basin number” and “specific flow rate”. In the specific flow rate database, the specific flow rate is recorded for each basin.

Next, the outflow amount estimation process will be described with reference to the drawings.
FIG. 62 is a flowchart showing the outflow amount estimation processing.
The input processing unit 40a receives river flow measurement data input from the river flow information system (river flow data 242), and sets the received data to “river flow measurement data” in the river flow measurement database. Register as a key (step Sd ₁₃ 1). Outflow amount estimation unit 364, a river flow measurement database with reference to the "basin No" as a key, also, the "catchment area" of Morphometry database referencing the "basin No" as a key (Step Sd 13 _2). Next, the outflow estimation unit 364 calculates the specific flow rate by dividing the river flow measurement data by the referenced basin area, and records it in the “specific flow” of the river flow measurement database using the basin No as a key (step Sd). ₁₃ 3). Further, the outflow amount estimating unit 364, "basin No" to the reference to the outflow index database as a key (Step Sd 13 _4), to create a scatter plot of the specific discharge and outflow index, the correlation between the outflow indicators and specific discharge Determine if there is any. When determining, the outflow amount estimation unit 364 refers to the value of the preset threshold value “S1” in the flow rate threshold value database, and if the correlation coefficient between the outflow index and the specific flow rate in the scatter diagram is equal to or greater than the threshold value S1. correlation Yes, it is determined that no correlation is less than the threshold value S1 (step _Sd 13 5). If it is determined that there is a correlation, the outflow amount estimating unit 364 calculates the regression equation between the outflow indicators and specific discharge (Step Sd 13 _6). Next, the outflow amount estimation unit 364 refers to the “outflow index” in the outflow index database using “basin number” as a key, calculates the specific flow rate for each basin based on the regression equation and the referenced outflow index, and calculates the specific flow rate. In the “specific flow rate” of the database, “basin number” is recorded as a key (step Sd ₁₃ 7). On the other hand, if it is determined that there is a correlation is no or negative correlation, for a review of the outflow index is needed (step Sd 13 _8), the process ends.
Since the data calculated by this process is a specific flow rate, it is necessary to multiply the basin area for each basin when calculating the spillage for each basin. Performed by the unit 32a.

As described above, the actual runoff amount used for runoff estimation includes not only the measured river runoff amount that is an actual measurement value, but also the annual river flow rate that is observed at a flow rate observation station that is an observation value. The outflow amount estimation processing performed by the outflow amount estimation unit 364 will be described using this observation value.
FIG. 63 is a diagram illustrating a data structure of data used for the outflow amount estimation processing. The observatory basin database shown in FIG. 1A has items including “basin No”, latitude “X”, longitude “Y”, and “precipitation” in the basin. Further, the river flow rate observation database shown in FIG. 2B includes items of “basin number”, “precipitation amount” for each basin, “river flow rate observation data”, and “runoff rate” (calculation result). In the river flow observation database, river flow observation data in a basin where river flow measurement data exists is registered, and the calculated runoff rate is recorded. The runoff rate database shown in FIG. 3C has items including “basin number” and “runoff rate”. The runoff rate database records each runoff rate (estimated result) for each basin.

Next, the outflow amount estimation processing based on the observation value will be described with reference to the drawings.
FIG. 64 is a flowchart showing an outflow amount estimation process based on the observed value.
The runoff amount estimation unit 364 refers to the basin division database, and converts the “basin No”, “X”, and “Y” of the basin where the observatory exists to the observatory basin database as “basin No”, “X”, and “Y”. "As a key. The input processing unit 40a receives precipitation data input from the weather information system (weather data 243), and registers the received data in the same observatory basin database with “X” and “Y” as keys. (Step Sd ₁₃ 11). The runoff estimation unit 364 refers to the observatory basin database using “basin No.”, “X” and “Y” as keys, integrates precipitation data over the entire basin, and calculates precipitation for each basin. To do. Next, the runoff amount estimation unit 364 records “Precipitation” in the river flow rate observation database using “basin number” as a key (step Sd ₁₃ 12). The input processing unit 40a receives the river flow observation data input from the river flow information system (river flow data 242), uses the received data as “river flow observation data” in the river flow observation database, and the basin number as a key. Registration is performed (step Sd ₁₃ 13). Next, the outflow estimation unit 364 refers to the river flow observation database using “basin No” as a key, and for the basin No in which the river flow observation data is input, the precipitation is divided by the river flow observation data and the runoff is calculated. The rate is calculated and recorded in the “flow rate” of the river flow rate observation database (step Sd ₁₃ 14). Further, the outflow amount estimation unit 364 refers to the outflow index database using “basin number” as a key (step Sd ₁₃ 15), creates a scatter diagram of the outflow rate and the outflow index, and correlates between the outflow index and the outflow rate. It is determined whether or not there is (step Sd ₁₃ 16). When determining, the outflow amount estimation unit 364 refers to “S1” in the flow rate threshold value database. If the correlation coefficient between the outflow index and the outflow rate in the scatter diagram is S1 or more, there is a correlation, and if it is less than S1, It is determined that there is no correlation. When it is determined that there is a correlation, the outflow amount estimation unit 364 calculates a regression equation between the outflow index and the outflow rate (step Sd ₁₃ 17). Next, the outflow amount estimation unit 364 refers to the outflow index database using “basin number” as a key, calculates the outflow rate for each basin based on the regression equation, and records it in the “outflow rate” of the outflow rate database (Step S Sd ₁₃ 18). On the other hand, if it is determined that there is no correlation or a negative correlation, the outflow index needs to be reexamined (step Sd ₁₃ 19), and the process is terminated.
Since the data calculated by this process is the runoff rate, when calculating the runoff for each basin, it is necessary to multiply by the precipitation for each basin. Performed by the unit 32a.

Next, the precipitation estimation process performed by the precipitation calculation unit 37 will be described.
FIG. 65 is a diagram showing a data structure of data used for precipitation estimation processing. The precipitation estimation database shown in FIG. (A) includes latitude “X”, longitude “Y”, altitude “H”, “precipitation”, “loss-corrected precipitation” and “spatial interpolation precipitation”. It consists of items, and “Precipitation” at the weather station is registered, and “Precipitation after spatial interpolation” in the measurement target area (multiple basins) is recorded. The precipitation threshold value database of FIG. (B) has an item consisting of “S2”. In S2, a threshold for determining whether there is a correlation between the altitude value of the weather station and the precipitation is set. The grid precipitation database in FIG. (C) includes latitude “X”, longitude “Y”, altitude “H”, and “estimated precipitation” (lattice DEM) in the measurement target area.

Next, precipitation estimation processing will be described with reference to the drawings.
FIG. 66 is a flowchart showing precipitation estimation processing.
The precipitation calculation unit 37 refers to the terrain database using “X” and “Y” as keys, and calculates the latitude X, longitude Y and altitude of the weather station and all the latitudes X and longitude Y in the measurement target area. “X” and “Y” are registered as keys in the quantity estimation processing database. Further, the input processing unit 40a receives the precipitation data of the weather station input from the weather information system (weather data 243), and the received data is transferred to “precipitation” in the precipitation estimation processing database, and “X”. And “Y” is registered as a key (step Sd ₁₄ 1). Next, the precipitation calculation unit 37 performs supplementary loss correction on the registered precipitation, calculates the loss-corrected precipitation, and records it in the “loss-corrected precipitation” in the precipitation estimation processing database ( Step Sd ₁₄ 2). The precipitation calculation unit 37 creates a scatter diagram of the altitude and the loss-corrected precipitation, and determines whether there is a correlation between the altitude and the loss-corrected precipitation. At the time of determination, the precipitation calculation unit 37 refers to a preset threshold “S2” in the precipitation threshold database, and whether the correlation coefficient between the altitude and the loss-corrected precipitation is equal to or greater than the threshold S2. It determines whether less than a threshold S2 (step _Sd 14 3). When the correlation calculation unit 37 determines that the correlation coefficient is greater than or equal to the threshold value S2, the precipitation calculation unit 37 determines that there is a correlation between the two, calculates a regression equation for determining elevation and loss-corrected precipitation, gradient) to extract (step _Sd 14 4). Next, the precipitation calculation unit 37 corrects the loss-corrected precipitation to a value of altitude 0 m based on the rate of increase / decrease (step Sd ₁₄ 5). Next, the precipitation calculation unit 37 performs spatial interpolation based on the corrected value, calculates precipitation at an altitude of 0 m (precipitation after spatial interpolation) for all X and Y in the measurement target area, It is recorded on the "X" and "spatial interpolation after precipitation" of rainfall estimation process database "Y" as a key (step Sd 14 _6). The input processing unit 40a receives DEM data input from the altitude value information system (DEM data 241), and registers the received DEM data in “X”, “Y”, and “H” of the grid precipitation database ( Step Sd ₁₄ 7). The precipitation calculation unit 37 obtains the precipitation according to the elevation value of the DEM data by multiplying the rate of increase / decrease by the elevation value, adds the precipitation after spatial interpolation to the multiplied result, and calculates the precipitation for each grid DEM in the target area. calculating the precipitation, as a key "X" and "Y", and records the "estimated precipitation" grid precipitation database (step Sd 14 _8).
On the other hand, in step Sd 14 _3, is less than the correlation coefficient threshold value S2, precipitation calculating unit 37 determines that no correlation between the altitude loss corrected precipitation (step Sd 14 _9), space Interpolation is performed to calculate precipitation for each grid, and “X” and “Y” are used as keys to record in the grid precipitation database “estimated precipitation” (step Sd ₁₄ 10).
Since the precipitation calculated by this process is a value for each grid DEM data, it is necessary to add up for each basin in order to calculate the outflow for each basin, but this process will be described later. This is performed by the rainfall recharge calculating unit 32a.

As described above, since the runoff amount (specific flow rate) per unit area in each basin and the precipitation amount (grid precipitation amount) corresponding to the grid DEM data are obtained, the calculation process performed by the rainfall recharge amount calculation unit 32a will be described.
FIG. 67 is a diagram showing a data structure of data used for the arithmetic processing. The grid estimator database shown in FIG. (A) includes “basin No.”, latitude “X”, longitude “Y”, “estimated precipitation”, “estimated runoff”, “estimated evapotranspiration” and “estimated recharge”. It has an item consisting of “amount”. In the grid estimation amount database, each grid estimation amount for each grid is recorded using the basin No, the latitude X, and the longitude Y as keys. Further, the estimated basin database shown in FIG. 5B includes items including “basin number”, “estimated precipitation”, “estimated runoff”, “estimated evapotranspiration”, and “estimated recharge”. The estimated amount database for each basin is recorded in the estimated basin database using “basin No” as a key.

FIG. 68 is a flowchart showing calculation processing performed by the rainfall recharge calculating unit 32a.
The rainfall recharge calculating unit 32a refers to the value of the basin division database for each basin No, and records the division data (latitude X and longitude Y) of the target basin in the lattice estimation amount database. Further, the rainfall recharge calculating unit 32a refers to “estimated precipitation” for each grid in the grid precipitation database using “X” and “Y” as keys, and records them in “estimated precipitation” in the grid estimated database. (Step Sd ₁₅ 1). Next, the rainfall recharge calculating unit 32a adds up the estimated precipitation for each grid for the entire basin for each basin No, and uses the “estimated precipitation” in the basin estimator database using the basin No as a key. (Step Sd ₁₅ 2). Next, the rainfall recharge calculating unit 32a refers to the “runoff rate” in the runoff rate database using the catchment area No as a key, and sets this as the runoff rate of all the grids in the catchment area. Alternatively, the rainfall recharge calculating unit 32a refers to the “specific flow rate” in the specific flow rate database using the basin number as a key and multiplies the area per grid to obtain the specific flow rate of all the grids in the basin ( Step Sd ₁₅ 3). Next, the rainfall recharge amount calculation unit 32a calculates an estimated outflow amount for each grid and an estimated outflow amount for each basin. When the runoff rate is used, the rainfall recharge calculating unit 32a multiplies the estimated precipitation amount for each grid by the runoff rate for each grid to calculate the estimated runoff amount for each grid, and the “estimated runoff amount” in the grid estimator database. To record. Also, the estimated precipitation for each basin is multiplied by the runoff rate for each basin to calculate the estimated runoff for each basin and record it in the “Estimated runoff” in the basin estimator database. If the estimated precipitation is a daily rainfall, an estimated runoff per day is calculated, and if it is a monthly rainfall, an estimated runoff per month is calculated. On the other hand, when calculating the estimated runoff amount based on the specific flow rate, the rainfall recharge amount calculation unit 32a records the specific flow rate for each grid in the “estimated runoff amount” of the grid estimated amount database. Further, the rainfall recharge amount calculation unit 32a refers to the basin area of the topographic measurement database using the basin number as a key, multiplies the specific flow rate to calculate the estimated outflow amount for each basin, and the integrated result is “ recording the estimated outflow "(step _Sd 15 4). When the specific flow rate is a specific flow rate per day, the estimated flow rate per day is calculated by multiplying the specific flow rate by (basin area / 100 × 60 × 60 × 24), and is the specific flow rate per month. In this case, the estimated outflow amount per month is calculated by further multiplying the number of days in the current month. Next, the rainfall recharge amount calculation unit 32a refers to “X” and “Y” in the grid estimated amount database using “basin number” as a key, and calculates evapotranspiration using the referenced “X” and “Y” as keys. see "potential evapotranspiration" processing database, it records the "estimated evapotranspiration" lattice estimator database (step Sd 15 _5). Next, the rainfall recharge calculating unit 32a adds up the estimated evapotranspiration for each grid for the entire basin for each basin No, and uses the basin no. (Step Sd ₁₅ 6). Next, the rainfall recharge calculating unit 32a calculates an estimated recharge amount for each basin according to (estimated precipitation amount for each basin−estimated evapotranspiration for each basin−estimated runoff amount for each basin). Record in “Estimated Evapotranspiration”. Further, the rainfall recharge amount calculation unit 32a calculates an estimated recharge amount for each lattice according to (estimated precipitation amount for each lattice−estimated evapotranspiration for each lattice−estimated outflow amount for each lattice). It is recorded in "rainfall recharge amount" of the estimated recharge amount "and rainfall recharge rate information database (step Sd 15 _7).

Thus, through a plurality of calculation and determination processes, precipitation, runoff, and recharge can be accurately calculated for each basin and for each grid based on quantitative data. In addition, this allows the total head calculation processing unit 34 to calculate the total head value based on the accurately calculated recharge amount for each lattice, so that the groundwater transfer route / transfer time calculation processing unit 35 calculates Based on the total water head value, it is possible to specify the groundwater transfer route and calculate the transfer time more accurately than in the past.
In the factor analysis described above, in the basin where the verification was made, the analysis factors that increase the factor loading of factor 1 include the average erosion height, Laplacian SD (landscape complexity), and factor loading of factor 2. The flow path shape ratio and the branching ratio R1 _{/ 2} were selected as analysis variables to be increased. The analysis variables selected are not limited to these because they may vary depending on the basin. Even if the basins are different, as described in detail in this embodiment, it is understood that a factor indicating the ease of water flow is extracted as factor 1 and a factor directly related to the difficulty of water flow is extracted as factor 2. Is done.
In the factor analysis, 11 items are selected as analysis variables. However, this is shown as an example of demonstration in the above-described embodiment, and is not limited to this number.

  The step of dividing the target area into a plurality of basins from the DEM data according to the present invention and performing the terrain measurement in the divided basins corresponds to the process of step SD10 performed by the terrain measurement unit 361. Further, the step of extracting a plurality of components having a correlation with the ease of water flow from the topographic measurement result according to the present invention corresponds to the process of step SD11 performed by the statistic processing unit 362. Further, the step of calculating the outflow index of the basin divided from the plurality of components according to the present invention corresponds to the process of step SD12 performed by the outflow index determination unit 363. Further, according to the present invention, the step of deriving a regression equation from the correlation between the outflow index of a part of the basin and the measured outflow amount, and the outflow of the basin divided from the derived regression equation and the outflow index of the divided basin The step of calculating the amount corresponds to the process of step SD13 performed by the outflow amount estimation unit 364.

DESCRIPTION OF SYMBOLS 100,100a Groundwater origin analysis system 110 Operation processing part 10 Ion concentration water quality information determination processing part 20 Isotope ratio determination processing part 30, 30a Groundwater transfer calculation processing part 31 Evapotranspiration amount calculation part 32, 32a Rain recharge amount calculation part 33 Pressure Head 0m setting unit 34 Total head calculation processing unit 35 Groundwater transfer path / transfer time calculation processing unit 40, 40a Input processing unit 50 Control storage processing unit 70 Storage unit 80 Output processing unit 90 Display unit 200, 200a Information input system 210 Water quality information data 220 Isotope information data 231 Remote sensing system 232 Rainfall information system 233 Map information system 234 Geological information system 36 Runoff calculation unit 37 Precipitation calculation unit 361 Topographic measurement unit 362 Statistical processing unit 363 Runoff index determination unit 364 Runoff amount Estimator 241 High information system (DEM data)
242 River flow information system (river flow data)
243 Weather Information System (Meteorological Data)

Claims (8)

A rain recharge calculation method for calculating rainfall recharge from runoff, precipitation, and evapotranspiration,
The step of calculating the outflow amount includes:
A first step of dividing the target area into a plurality of basins from the terrain data, and measuring terrain in the divided basins;
A second step of extracting a plurality of factors having a correlation with the ease of water flow from the topographic measurement results;
A third step of calculating an outflow index of the divided basin from the plurality of factors;
A fourth step of deriving a regression equation from a correlation between an outflow index of a part of the basin and the measured outflow amount;
A fifth step of calculating the outflow amount of the divided basin from the derived regression equation and the outflow index of the divided basin;
A rain recharge calculation method comprising: The third step includes
A first factor having a positive correlation with water flowability and a second factor having a negative correlation with water flowability are extracted, and a factor score for each factor of the divided watershed is calculated and calculated. The divided watersheds according to the factor scores that have been divided are classified into a predetermined number of groups for each factor, each group is assigned a preset score for each factor, and the given score and each The rain recharge calculation method according to claim 1, wherein an outflow index of the divided basin is calculated according to a contribution ratio of the factor. A terrain measurement unit that divides the target area into a plurality of basins from the terrain data, and measures terrain in the divided basins;
A statistical processing unit that extracts a plurality of factors having a correlation with the ease of water flow from the topographic measurement results;
An outflow index determination unit for calculating an outflow index of the divided basin from the plurality of factors;
Deriving a regression equation from the correlation between the outflow index of a part of the basin and the measured outflow amount,
An outflow amount estimation unit for calculating the outflow amount of the divided basin from the derived regression equation and the outflow index of the divided basin;
A rainfall recharge calculating unit, comprising: a runoff amount calculating unit that calculates a rain recharge amount based on the calculated outflow amount. The outflow index determination unit
A first factor having a positive correlation with water flowability and a second factor having a negative correlation with water flowability are extracted, and a factor score for each factor of the divided watershed is calculated and calculated. The divided basin according to the factor score is classified into a predetermined number of groups for each factor, a preset score is assigned to each group for each factor, and the given score and each The rainfall recharge calculating unit according to claim 3, wherein an outflow index of the divided basin is calculated according to a contribution ratio of the factor. A step of calculating the origin of groundwater from the degree of coincidence of the ratios of ion concentrations in the ion concentration data at a plurality of points stored in the storage unit by the ion concentration determination processing unit;
A step in which the isotope ratio determination processing unit calculates the recharge height from the degree of coincidence of the isotope ratios in the isotope ratio data stored in the storage unit;
A step of calculating an evapotranspiration amount for each region in the satellite image data of the vegetation area stored in the storage unit by the evapotranspiration unit;
A step in which the outflow amount calculation unit calculates the outflow amount;
A step of calculating the amount of seepage water from the amount of evapotranspiration, the amount of precipitation stored in the storage unit, and the amount of runoff by the rainfall recharge amount calculation unit;
A step of calculating a position of the groundwater level 0 m for each area from satellite image data indicating a river area stored in the storage unit by the pressure head 0 m setting unit;
A step in which a total head calculation processing unit calculates a head value of the region from the amount of osmotic water and elevation information of each point;
A groundwater transfer route / transition time calculation processing unit calculating a groundwater transfer route and a transfer time from the distribution of the head value, and a groundwater origin analysis method comprising:
The step of calculating the outflow amount includes:
A first step of dividing the target area into a plurality of basins from the terrain data, and measuring terrain in the divided basins;
A second step of extracting a plurality of factors having a correlation with the ease of water flow from the topographic measurement results;
A third step of calculating an outflow index of the divided basin from the plurality of factors;
A fourth step of deriving a regression equation from a correlation between an outflow index of a part of the basin and the measured outflow amount;
A fifth step of calculating the outflow amount of the divided basin from the derived regression equation and the outflow index of the divided basin;
A groundwater origin analysis method characterized by comprising: An ion concentration determination processing unit for calculating the origin of groundwater from the degree of coincidence of the ion concentration ratios in the ion concentration data at a plurality of points stored in the storage unit;
An isotope ratio determination processing unit that calculates the recharge height from the degree of coincidence of the isotope ratios in the isotope ratio data of the plurality of points stored in the storage unit;
An evapotranspiration calculating unit for calculating an evapotranspiration amount for each region from the satellite image data of the vegetation area stored in the storage unit;
An outflow amount calculation unit for calculating an outflow amount;
A rainfall recharge calculating unit that calculates an infiltrated water amount from the evapotranspiration, a precipitation amount stored in a storage unit, and the outflow amount;
A pressure head 0m setting unit for setting the position of the groundwater level 0m for each region from the satellite image data indicating the river area stored in the storage unit;
A total head calculation processing unit for calculating the head value of the region from the amount of osmotic water and elevation information at each point;
A groundwater origin analysis system comprising a groundwater transition route and a transition time calculation processing unit for calculating a groundwater transition route and a transition time from the distribution of the head value,
The outflow amount calculation unit
A terrain measurement unit that divides the target area into a plurality of basins from the terrain data, and measures terrain in the divided basins;
A statistical processing unit that extracts a plurality of factors having a correlation with the ease of water flow from the topographic measurement results;
An outflow index determination unit for calculating an outflow index of the divided basin from the plurality of factors;
Deriving a regression equation from the correlation between the outflow index of a part of the basin and the measured outflow amount,
An outflow amount estimation unit for calculating the outflow amount of the divided basin from the derived regression equation and the outflow index of the divided basin;
A groundwater origin analysis system characterized by comprising: To the computer in the groundwater origin analysis system,
Calculating the origin of groundwater from the degree of coincidence of the ratios of ion concentrations in the ion concentration data at a plurality of points stored in the storage unit;
Calculating the recharge height from the degree of coincidence of the isotope ratios in the isotope ratio data of a plurality of points stored in the storage unit;
Calculating the amount of evapotranspiration for each region from the satellite image data of the vegetation area stored in the storage unit;
Calculating a spill amount;
Calculating the amount of osmotic water from the amount of evapotranspiration, the amount of precipitation stored in the storage unit, and the amount of runoff;
Setting the position of the groundwater level 0 m for each region from the satellite image data indicating the river region stored in the storage unit;
Calculating the water head value of the region from the amount of osmotic water and elevation information of each point;
Calculating groundwater transfer route and transfer time from the distribution of the head value;
A groundwater origin analysis program that executes
The step of calculating the outflow amount includes:
Dividing the target area into a plurality of basins from the terrain data, and performing terrain measurement in the divided basins;
A second step of extracting a plurality of factors having a correlation with the ease of water flow from the topographic measurement results;
A third step of calculating an outflow index of the divided basin from the plurality of factors;
A fourth step of deriving a regression equation from the correlation between the outflow index of a part of the basin and the actually measured outflow amount;
A fifth step of calculating an outflow amount of the divided basin from the derived regression equation and an outflow index of the divided basin;
The groundwater origin analysis program characterized by having.   The computer-readable recording medium which recorded the program of Claim 7 made to be performed by the computer in a groundwater origin analysis system.