KR101543722B1 - Method of numerical verification of hyporheic zone depth estimation using streambed temperature - Google Patents

Abstract

The present invention provides a method for measuring a depth of a hyporheic zone of a stream bed, comprising: a temperature measurement step of measuring a temperature for each depth of a stream bed for measuring the depth of a hyporheic zone of the stream bed; a step of estimating a shape and a size of hyporheic flux of the stream bed; a quantitative analysis step of quantitatively analyzing an interaction between underground water and the surface water through the measured temperature; and a depth of the hyporheic zone calculation step of calculating the depth of the hyporheic zone through the measured temperature. Therefore, the method reduces time consumed for estimating the depth of the hyporheic zone and is simple and has excellent field applicability. Moreover, the method enables a user to quantitatively analyze a water resource quantity of the available underground water and the available surface water and to prevent, in advance, contamination of the underground water and effectively manage the contamination of the underground water.

Description

TECHNICAL FIELD [0001] The present invention relates to a method for measuring a depth of a hyperic-

Field of the Invention [0002] The present invention relates to the field of environmental technology, and more particularly, to a method for measuring the depth of a hyperic rock in a river.

In modern society, as climate change and environmental pollution become serious, stable water resource availability becomes increasingly difficult.

Groundwater is stable to external changes compared to surface water and has a characteristic that the change is slow.

These groundwater resources are becoming an essential source of water for human survival, and their importance is increasing.

On the other hand, hypericons mean active interactions (exchange, storage, etc.) between groundwater and surface water.

By estimating the depth of this hyperic - zon, the amount of available groundwater and surface water can be quantitatively assessed and a method for recovering contaminated groundwater can be sought.

Conventionally, there is a method of tracer test using chlorine, bromine, rhodamine, etc. in order to obtain the depth of hyperic.

In order to perform such a tracer test method, consideration must be given to various factors such as the choice of the tracer, the concentration, the measuring range, the sampling and analysis method, the physical, chemical, biological properties and toxicity of the tracer.

Therefore, the above method has a lot of points to consider, so it takes a long time to track the depth of the Hyperic-zon and has a disadvantage that it is troublesome to work.

In addition, there is a disadvantage that the accuracy of the resultant value is deteriorated because an error may occur among the respective items.

SUMMARY OF THE INVENTION It is an object of the present invention to solve the above problems and to provide a method and apparatus for quantitatively analyzing the amount of groundwater and surface water that can be used and which has a short time required for estimating the depth of hyperic- And it is an object of the present invention to provide a method for measuring the depth of a hyperic rock in a river that can prevent contamination of groundwater and effectively manage it.

In order to solve the above problems, the present invention provides a method for measuring a depth of a river, comprising: a temperature measuring step of measuring a depth of a river by depth; Estimating the shape and size of the hyperic flux of the stream; A quantitative analysis step of quantitatively analyzing the interaction between the ground water and the surface water through the measured temperature; And calculating a depth of the hyperic-zone based on the measured temperature. The present invention also provides a method for measuring the depth of a hyperic-zone depth of a river.

It is preferable that the hyperlite depth calculating step is calculated by the following equation (1).

[Equation 1]

In Equation (1) above,

ρ: density of particles (kg / m ³ )

C: Heat capacity of the soil (J / k ° C)

T: Temperature (캜)

: 유효 열전도도(W/m℃)

: Effective thermal conductivity (W / m ° C)

: (유체의 흐름이없는 경우) 초기 열전도도(W/m℃)

: (Without fluid flow) Initial thermal conductivity (W / m ° C)

: 유체의 열전도도(W/m℃)

: Thermal conductivity of fluid (W / m ° C)

: 입자의 열전도도(W/m℃)

: Thermal conductivity of particles (W / m ° C)

β: thermal diffusivity (m)

n: Porous (-)

ρ _f : density of fluid (kg / m ³ )

C _f : Specific heat of fluid (J / k ° C)

V _f : vertical fluid velocity (m / s)

z: depth (m)

t: Time (s)

The quantitative analysis step is preferably calculated by the following equations (2) and (3).

&Quot; (2) "

&Quot; (3) "

In the above equations (2) and (3)

t: Time (s)

x: Length in the stream direction (m)

C: Concentration of stream (mg / L)

C _S : Concentration of storage zone (mg / L)

C _L : Concentration of groundwater (mg / L)

Q: Volumetric flow of stream (m ³ / s)

q _L ⁱⁿ : Inflow range of groundwater per unit area of river (m ³ / s / m)

D: Vertical diffusion coefficient of stream (m ² / s)

A: Cross-sectional area of stream (m ² )

A _S : sectional area of the storage zone (m ² )

: 저장교환계수(S^-1)

: Storage Exchange Coefficient (S ^-1 )

λ: the first rate constant (s ^-1 ) representing the net absorption of the reactive solute by biological processes in the stream flow

λ _S is the first rate constant (s ^-1 ) representing the net absorption of the reactive solute by the chemical process of the stream flow,

It is preferable that the quantitative analysis step is calculated by the following equations (4) and (5).

&Quot; (4) "

&Quot; (5) "

And a comparison step of comparing the calculated hyperbolic depth with the field data value after the hyperbolic depth calculation step.

After the comparing step, it is preferable to repeat the step of estimating the shape and size of the hyperic flux and the step of calculating the hyperic-kernel depth.

And a sensitivity evaluation step of calculating a sum of squared differences (SSD) value and evaluating the sensitivity after the hypersensitive depth calculation step.

The present invention provides a method for estimating the depth of a hyperic-zon in a short time, simple, excellent in field application, quantitatively analyzing the amount of groundwater and surface water that can be used, preventing contamination of groundwater, This paper presents a method for measuring the depth of a hyperic rock in a river.

1 to 4 illustrate a method for measuring the depth of a hyperic rock in a river according to the present invention,
BRIEF DESCRIPTION OF THE DRAWINGS FIG. 1 is a block diagram showing a hyperic area of a river. FIG.
2 is a conceptual view of a hyperic flux;
3 is a schematic view of a hyperic flux for heat transfer analysis.
Fig. 4 shows a kind of a hyperic flux shape. Fig.
FIGS. 5 to 14 illustrate an experiment for confirming the validity of the method for measuring the depth of hyperic-zone of a river according to the present invention,
Fig. 5 is an on-the-spot map of an experiment conducted to confirm the validity of the hyperlick-zen depth measurement method.
FIG. 6 is a data condition used to verify the validity of the hyperic-zon depth measurement method, where a is a virtual initial condition, and b is a temperature-dependent temperature graph of the river according to a virtual boundary condition.
7 is a graph showing a temperature distribution of a river when the hyperic shape is a triangular shape.
FIG. 8 is a three-dimensional graph showing the sensitivity evaluation result of the triangular shaped hyperic flux. FIG.
9 (a) is a sensitivity evaluation result according to the hyperic flux depth and shape, and b is a graph showing a sensitivity evaluation result according to the hyperic flux size and shape.
10 is a configuration diagram for examining the effect of a hyperic flux shape on the hyperic flux depth;
FIG. 11 is a graph showing the temperature distribution of depths of a river in a measurement area. FIG.
12A is a graph showing the temperature distribution of the initial condition by the interpolation method and b is a graph showing the temperature distribution of the boundary condition by the interpolation method.
13 is a graph showing the temperature distribution of a hyperic flux having a triangular shape and having Vf, max = -0.4 mm / min and D _H = 0.116 m.
14 is a graph showing the distribution of trace substances by depth of hyperlyzone in order to compare the method of the present invention with the tracer test method.

Hereinafter, embodiments of the present invention will be described in detail with reference to the accompanying drawings.

The method of measuring the depth of a hyper-rain zone of a river according to the present invention includes: a temperature measurement step of measuring a depth of a river according to a depth of a river to measure a depth of a hyper-rain zone; Estimating the shape and size of the hyperic flux of the stream; A quantitative analysis step of quantitatively analyzing the interaction between groundwater and surface water through measured temperatures; And a hyperic-yn depth calculating step of calculating a hyperic-yn depth through the measured temperature.

That is, the measurement method of the present invention can more easily estimate the hyperic-kernel depth by using the stream temperature measured in the field and the shape of the hyperic flux, as compared with the tracker test, which is a conventionally used hyperic-depth measuring method.

Therefore, the following advantages can be obtained.

First, there is an advantage that the operation of estimating the depth of hyperic - zon is simple and quick.

Second, it has a merit that it can be easily applied in the field because the matters to be considered in comparison with the conventional tracker test are simple.

Third, since the measurement is made using only the shape of the stream temperature data and the hyperic flux measured in the field, there is less possibility of error as compared with the conventional tracker test.

Therefore, there is an advantage that the reliability and accuracy of the result value for the depth estimation of hyperic-zon are improved.

Fourth, it is possible to quantitatively analyze the amount of available groundwater and surface water resources through a simple and accurate measurement method, and to prevent contamination of groundwater and to effectively manage it.

Therefore, it is possible to obtain an effect of being highly desirable from the environmental point of view.

More specifically, the method for measuring the depth of a hyperic-rain of a river according to the present invention includes a step of measuring the temperature at a depth of a river in the field, that is, at a surface temperature of 1 cm, 10 cm, 20 cm, 30 cm, 40 cm, .

In addition, a step of estimating the shape and size of the hyperic flux is performed together.

The data obtained through the above steps are used to quantitatively analyze the interactions between groundwater and surface water, and to calculate the hyperic-zon depth.

The present invention is based on the fact that the temperature distribution by the depth of a river is influenced by the hyperic flux, and the depth of the hyperic zone can be measured by using this.

Also, the measured temperature data can be calculated using a conduction-advection-dispersion equation (CAD).

The above CAD expression is the expression (1) proposed by the present invention, and the expression (1) is calculated as follows.

는 유효 열전도도(W/m℃),

는 (유체의 흐름이없는 경우) 초기 열전도도(W/m℃),

는 유체의 열전도도(W/m℃),

는 입자의 열전도도(W/m℃), β는 열분산성(m), n는 다공성(-), ρ_f는 유체의 밀도(kg/m³), C_f는 유체의 비열(J/k℃), V_f는 수직유체속도(m/s), z는 깊이(m), t는 시간(s)을 의미한다.In the above equation (1), ρ is the density of the particles (kg / m ³ ), c is the heat capacity of the soil (J / k ° C), T is the temperature

(W / m < 0 > C),

(In the absence of fluid flow), initial thermal conductivity (W / m ° C),

Is the thermal conductivity (W / m ° C) of the fluid,

(M), n is the porosity (-), ρ _f is the density of the fluid (kg / m ³ ), C _f is the specific heat of the fluid (J / k ° C), V _f is the vertical fluid velocity (m / s), z is depth (m) and t is time (s).

FIG. 2 is a conceptual diagram of a hyperic flux, and FIG. 3 is a schematic diagram of a hyperic flux for heat transfer analysis.

As shown in FIG. 2, the initial condition and the boundary condition in Equation (1) are indispensable factors, and these conditions can be obtained according to the depth distribution of the depths of the rivers collected in the field according to depth and time .

On the other hand, the step of quantitatively analyzing the interaction between the groundwater and the surface water is calculated by the following equations (2) and (3).

는 저장교환계수(S^-1), λ는 하천 흐름의 생물학적 과정에 의해 반응성 용질의 순흡수를 나타내는 첫번째 속도상수(s^-1) λ_S는 하천 흐름의 화학적 과정에 의해 반응성 용질의 순흡수를 나타내는 첫번째 속도상수(s^-1)를 의미한다.Where C is the concentration of the stream (mg / L), C _S is the concentration of the storage zone (mg / L) ), C _L is the groundwater concentration (mg / L), Q is the volumetric flow of the river (m ³ / s), q _L ⁱⁿ is the groundwater inflow range (m ³ / s / (M ² / s), A is the cross-sectional area of the stream (m ² ), A _s is the cross-sectional area of the storage zone (m ² )

(S ^-1 ), where λ is the first rate constant (s ^-1 ) that represents the net uptake of the reactive solute by the biological process of _the stream flow, λ _{S is} the net absorption of the reactive solute by the chemical process of the stream flow Means the first rate constant (s ^-1 ) that represents.

Equations (2) and (3) are simplified by the following equations (4) and (5), assuming that the flow rate near the hypersonic zone is small and the distance between the point where the tracer material is injected and the measurement point is short .

는 하천의 물이 하이퍼릭 영역에서 교환되는 속도를 의미한다.In Equations 4 and 5,

Means the rate at which water in the stream is exchanged in the hyperic area.

And Equations (4) and (5) above can be associated with the hyperic flux by Equation (6).

In Equation (6) above,

q _s means the flow of the storage-exchange, ie the average flux of water through the Hyperion Zone per unit length of the stream.

A cross-sectional area _s of the storage zone is calculated from the depth d _s of the hyper rikjon, and to a depth d _s of the hyper rikjon may be computed through the equation (7).

In Equation (7), d _s is the depth (m) of the hyperic zone, w is the width of the stream (m), and n is the porosity of the sediment (-).

In addition, in the present invention, it is preferable that the comparing step of comparing the calculated hyperic-y'z depth with the field data value is further performed after the hyperic-yin depth calculating step.

After the comparison step, the step of estimating the shape and the size of the hyperic flux and the step of calculating the hyperic-zon depth are repeated (Fig. 2).

After the hypersensitive zone depth calculation step, it is preferable that a sensitivity evaluation step of calculating a sum of squared differences (SSD) value to evaluate the sensitivity is performed.

Since the hyperic flux is composed of two parameters, namely the shape and size of the hyperic flux, the SSD value is measured using the squared difference between the depth of the hyperic zone and the flux of the hyperic zone.

Hereinafter, an experimental example for examining the validity of the measurement method presented in the present invention will be described.

In order to evaluate the suitability of the depth measuring method of the Hyperic-zon proposed in the present invention, the hypothetical initial condition shown in FIG. 6 (a) and the hypothetical boundary condition shown in FIG. 6 (b) 1 < / RTI >

Fig. 7 shows the temperature distribution of the triangular hyperplastic flux at the maximum velocity V _{f =} 0.05 m / min and the depth D _h = 0.1 m in the imaginary initial and boundary conditions.

The point on the graph means the SSD value.

Table 1 shows the parameters of Equation (1).

The initial thermal conductivity was calculated using the fluid and particle conductivity, and the porosity of Table 1 is 1.927 W / m ° C, which is consistent with the porosity of the saturated sediments reported in the literature.

Since the SSD value depends on the size of the high flux, in order to investigate the size of the hyperic flux that minimizes the SSD value, the SSD value of the triangular shape according to the size of the hyperic flux is shown in Table 2, The result of substitution into the CAD formula is shown in Fig.

As shown in FIGS. 9A and 9B, it can be seen that the sensitivity of the SSD to the depth of the hyperbolic zone is greater than the speed of the hypermic flux regardless of the hyperic shape.

This result is a result of demonstrating the validity of the method of representing the shape of the hyperic-zon than the speed of the hyperic flux.

On the other hand, the effect of the hyperic flux shape on the river depth was evaluated.

For this purpose, a triangular hyperplastic flux having a condition of Vf.max = 0.005 m / min and DH = 0.10 m is calculated according to Equation (1) of the present invention and a comparison with the temperature distribution of another hyperplastic flux shape is made .

FIG. 3 shows that the size of hyperic zon, that is, the surface area, decreases as the depth of the river deepens. FIG. 4 shows the shape of hyperic fluxes assumed in the present invention, that is, spendral, triangle, cosine, a quarter of an ellipse Lt; / RTI >

FIG. 10 shows a process of examining the influence of the hyperic flux shape according to the optimal hyperic-zone depth, and the results of the investigation are shown in Table 3. [

As a result of the investigation, it can be seen that the depth and velocity of hyperic is decreased as the hyperic shape changes in order of spendral, triangle, cosine, ellipse.

However, as a result of calculating the hyperfine fluxes of different shapes by the equation (1), it can be confirmed that the effect of the hyperflex flux shape on the hyperfine depth is not large.

This is because the shape of the hyperic flux of the river at the site to be measured is generally difficult to grasp, so that the method proposed in the present invention is considered to be advantageous.

That is, in the present invention, although it is hard to know the shape of the hyperic flux, it is possible to estimate the depth of the hyperic zone in a relatively accurate range through a rough assumption.

Next, the depth of the Hyperic-zon was calculated by applying the measurement method of the present invention to the actual field.

The field region is as shown in Fig. 5, and the temperature distribution of the field region is as shown in Fig.

Assuming various hyperic flux shapes, the depth of the hyperic zone was calculated using the equation (1) proposed by the present invention, that is, a CAD equation.

As a result of the sensitivity evaluation, it can be confirmed that the SSD value calculated by each shape is similar to the actual value.

The graph shown in Fig. 12 is shown by interpolation from the temperatures at which initial and boundary conditions are measured.

The hyperic zone depth according to different hypermic flux shapes is shown in Table 4, and the result of calculating the triangular hypermic flux by Equation (1) is as shown in FIG.

FIG. 14 also shows the distribution of trace substances by depth of hyperic-zone in order to compare the method of the present invention with the conventional tracker test method.

As a result of the comparison, the same prediction results as those of the present invention were shown, and the results showed that the measurement method according to the present invention can be predicted in a relatively narrow range.

As described above, the method of estimating the hyperic-kernel depth in the present invention can obtain more accurate results than the conventional tracker test method, and it is advantageous that the measurement operation is relatively easy since it is the only method requiring only the temperature distribution.

It will be apparent to those skilled in the art that various modifications and variations can be made in the present invention without departing from the spirit or scope of the invention as defined in the appended claims. It is to be understood that both the technical idea and the technical spirit of the invention are included in the scope of the present invention.

Claims (7)

A temperature measuring step of measuring the depth of the river in order to measure the depth of the hyperic zone of the stream;
Estimating the shape and size of the hyperic flux of the stream;
A quantitative analysis step of quantitatively analyzing the interaction between the ground water and the surface water through the measured temperature;
And a hyperic-zoned depth calculating step of calculating a hyperic-zoned depth through the measured temperature
Wherein the method comprises the steps of: The method according to claim 1,
The hyperic-kernel depth calculation step
The method according to claim 1, wherein the depth of the hyperplane is measured by the following equation (1).
[Equation 1]

In Equation (1) above,
ρ: density of particles (kg / m ³ )
C: Heat capacity of soil (J / k ° C)
T: Temperature (캜)

: Effective thermal conductivity (W / m ° C)

: (Without fluid flow) Initial thermal conductivity (W / m ° C)

: Thermal conductivity of fluid (W / m ° C)

: Thermal conductivity of particles (W / m ° C)
β: thermal diffusivity (m)
n: Porous (-)
ρ _f : density of fluid (kg / m ³ )
C _f : Specific heat of fluid (J / k ° C)
V _f : vertical fluid velocity (m / s)
z: depth (m)
t: Time (s) The method according to claim 1,
The quantitative analysis step
(2) and (3): " (2) "
&Quot; (2) "

&Quot; (3) "

In the above equations (2) and (3)
t: Time (s)
x: Length in the stream direction (m)
C: Concentration of stream (mg / L)
C _S : Concentration of storage zone (mg / L)
C _L : Concentration of groundwater (mg / L)
Q: Volumetric flow of stream (m ³ / s)
q _L ⁱⁿ : Inflow range of groundwater per unit area of river (m ³ / s / m)
D: Vertical diffusion coefficient of stream (m ² / s)
A: Cross-sectional area of stream (m ² )
A _S : sectional area of the storage zone (m ² )

: Storage Exchange Coefficient (S ^-1 )
λ: the first rate constant (s ^-1 ) representing the net absorption of the reactive solute by biological processes in the stream flow
λ _S is the first rate constant (s ^-1 ) representing the net absorption of the reactive solute by the chemical process of the stream flow, The method of claim 3,
The quantitative analysis step
(4) and (5): " (5) "
&Quot; (4) "

&Quot; (5) "

The method according to claim 1,
After the hyperic-zoned depth calculation step,
A comparison step of comparing the calculated hyperbolic depth and the field data value;
And measuring the depth of the hyper-rain zone in the stream. 6. The method of claim 5,
After the comparing step,
Wherein the step of estimating the shape and size of the hyperic flux and the step of calculating the hyperic-kernel depth are repeated. The method according to claim 1,
After the hyperic-zoned depth calculation step,
A sensitivity evaluation step of calculating a sum of squared differences (SSD) value to evaluate the sensitivity;
And measuring the depth of the hyper-rain zone in the stream.

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