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翻訳と辞書　辞書検索 [ 開発暫定版 ] スポンサード リンク ZOOMQ3D ： ウィキペディア英語版 ZOOMQ3D ZOOMQ3D is a numerical finite-difference model, which simulates groundwater flow in aquifers. The program is used by hydrogeologists to investigate groundwater resources and to make predictions about possible future changes in their quantity and quality. The code is written in C++, an object-oriented programming language and can compile and run on Windows and Unix operating systems. == Groundwater flow equation == ZOOMQ3D applies a quasi-three-dimensional finite-difference approximation to the general three-dimensional governing partial differential groundwater flow equation: :$\backslash frac\; \backslash left(K\_\; \backslash frac\; \backslash right)\; +\; \backslash frac\; \backslash left(K\_\; \backslash frac\; \backslash right)\; +\; \backslash frac\; \backslash left(K\_\; \backslash frac\; \backslash right)\; =\; S\_\; \backslash frac\; -\; q$ where: *$\backslash phi(x,y,z,t)$ is the potentiometric head at a point $(x,\; y,\; z)$ and time $(t)$ (L) *$K\_$, $K\_$ and $K\_$ are the values of hydraulic conductivity along the ''x'', ''y'', and ''z'' coordinate axes (LT−1) *$q$ is a volumetric flux per unit volume representing sources and/or sinks of water, where ''negative'' values are abstractions, and ''positive'' values are injections (T−1) and, *$S\_$ is the specific storage of the porous material (L−1) This equation is derived by considering a flow balance for an infinitesimally small volume element located anywhere within a body of saturated aquifer. A number of assumptions underlie this equation. First, the fluid is assumed to be of constant density; this allows the flow balance to be a consequence of mass conservation within the element. Next, the Cartesian coordinate system is aligned with the principal axes of the hydraulic conductivity tensor; this avoids the need for cross derivatives. A model, based on the above equation, incorporating appropriate boundary and initial conditions, would be truly three-dimensional. ZOOMQ3D takes a simplifying approach to the solution of the three-dimensional equation by recognising that in many aquifers it is possible to identify a layered structure. If the layers are aligned parallel to the horizontal coordinate axes, then the three-dimensional equation can be integrated vertically across the layer to produce an equation which describes the flow within a layer and its interactions with adjacent layers. Such an equation is: :$\backslash frac\; \backslash left(T\_\; \backslash frac\; \backslash right)\; +\; \backslash frac\; \backslash left(T\_\; \backslash frac\; \backslash right)\; =\; S\_\; \backslash frac\; -\; q\; -\; L\_\backslash mathrm\; +\; L\_\backslash mathrm$ where: *$h$ is the potentiometric head within a layer (L) *$t,$ is time (T) *$T\_$ and $T\_$ are the values of transmissivity along the ''x'' and ''y'' coordinate axes (L2T−1) *$q$ is a volumetric flux per unit plan area representing sources and/or sinks of water, where ''negative'' values are abstractions, and ''positive'' values are injections (LT−1) *$S$ is the storage coefficient of the porous material (L0) and, *$L$above and $L$below are leakage rates from layers above and below (LT−1) 抄文引用元・出典: フリー百科事典『 ウィキペディア（Wikipedia）』 ■ウィキペディアで「ZOOMQ3D」の詳細全文を読む スポンサード リンク 翻訳と辞書 : 翻訳のためのインターネットリソース Copyright(C) kotoba.ne.jp 1997-2016. All Rights Reserved.