为什么不能波模型模型风暴潮?- 江南体育网页版- - - - -地球科学堆江南电子竞技平台栈交换 最近30从www.hoelymoley.com 2023 - 07 - 08 - t21:31:55z //www.hoelymoley.com/feeds/question/5377 https://creativecommons.org/licenses/by-sa/4.0/rdf //www.hoelymoley.com/q/5377 9 为什么不能波模型模型风暴潮? user4624937 //www.hoelymoley.com/users/2645 2015 - 08 - 15 - t07:01:08z 2015 - 08 - 18 - t01:56:11z < p >我发现这个好模块< a href = " http://www.meted.ucar.edu/oceans/wavewatch3/navmenu.htm " rel = " noreferrer " > < / >在当场,WAVEWATCH波模型的概述。,在引言部分,提到WAVEWATCH不能风暴潮模型或海啸。这是适用于所有第三代模型吗?源项可以添加到能量平衡方程模型这些现象? < / p > //www.hoelymoley.com/questions/5377/-/5385 # 5385 13 由milancurcic回答为什么不能波模型风暴潮模型? milancurcic //www.hoelymoley.com/users/192 2015 - 08 - 15 - t21:43:46z 2015 - 08 - 18 - t01:56:11z < p >是的。光谱波模型不能模型风暴潮,因为波能量平衡方程,他们整合并不描述与风暴潮相关的物理过程。< / p >

Wave models solve the wave energy balance equation:

$$ \dfrac{\partial E}{\partial t} + \dfrac{\partial (c_gE)}{\partial x} + \dfrac{\partial (\dot{k}E)}{\partial k} + \dfrac{\partial (\dot{\theta} E)}{\partial \theta} = \rho_w g\sum S_i(x,k,\theta) $$ where the terms on the LHS represent local change in time and advection of energy in geographical ($x$), wavenumber ($k$), and directional ($\theta$) space, respectively. The source terms $S_i$ on the RHS determine the growth and decay of wave energy due to wind input, wave dissipation, and non-linear wave-wave interactions.

While mean water depth, wind forcing, and background Eulerian currents all affect the evolution of wave energy, the wave energy balance equation only solves for the statistical distribution of wave energy and its change in time. It does not provide information about the change of mean water level or Eulerian currents. The simplest equation set necessary to explicitly model surge are the single-layer (2-D) shallow water equations:

$$ \dfrac{d\mathbf{u}}{dt}=-g\nabla\eta + \dfrac{1}{\rho_w} \dfrac{\partial \boldsymbol{\tau}}{\partial z} $$

$$ \dfrac{\partial \eta}{\partial t} = -\nabla \cdot (\mathbf{u}(H+\eta)) $$ where $\mathbf{u}$ is the Eulerian velocity and $\eta$ is the displacement from the mean water level $H$. $\nabla$ is the horizontal gradient operator. $\dfrac{\partial \boldsymbol{\tau}}{\partial z}$ is the vertical stress gradient that forces the flow - essentially the difference between surface and bottom stresses. The momentum equation describes how the flow velocity changes due to horizontal pressure gradient and surface forcing (stress). The mass continuity equation describes how the water elevation changes due to divergence of the flow. For spatial scales larger than 10 km or so, Earth's rotation becomes important and the RHS of the momentum equation must include the Coriolis acceleration.

Another requirement for the model to simulate storm surge is to allow for wetting and drying. What this means is that the land cells, which are originally above mean water level, and thus not part of the model solution, can become wet once the water level reaches their height and "submerges" them. These grid cells then become part of the model solution. While this may sound obvious and physically intuitive, implementing a wetting-and-drying scheme in a model is a non-trivial challenge regarding software design.

When the wave and surge models are coupled, the Eulerian velocity field $\mathbf{u}$ is mainly forced by wave dissipation, and less by wind directly. The surface elevation changes in response, and together with Eulerian velocity feeds back to the wave model.

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