CMS-Flow:Hydro Eqs

Governing Equations

The depth-averaged 2-D continuity equation may be written as

${\frac {\partial h}{\partial t}}+\nabla \cdot (h\mathbf {U} )=S$

(1)

where $h$ is the total water depth $h=\zeta +\eta$, $\eta$ is the water surface elevation, $\zeta$ is the still water depth, $\mathbf {U} =\left({{U}_{1}},{{U}_{2}}\right)$ is the depth-averaged current velocity, $S$ is a source term due to precipitation and evaporation, and $\nabla =\left({{\nabla }_{1}},{{\nabla }_{2}}\right)$ is the divergence operator.

The momentum equation can be written as

${\frac {\partial (h{{U}_{i}})}{\partial t}}+\nabla \cdot (h\mathbf {U} {{U}_{i}})-\mathbf {BU} =-gh{{\nabla }_{i}}\eta +\nabla \cdot \left({{\nu }_{t}}h\nabla {{U}_{i}}\right)+{\frac {1}{\rho }}\left({{\tau }_{wi}}+{{\tau }_{Si}}-{{\tau }_{bi}}\right)$

(2)

where $g$ is the gravitational constant, $\mathbf {B} =\left({\begin{matrix}0&{{f}_{c}}\\-{{f}_{c}}&0\\\end{matrix}}\right)$ where $f_{c}$ is the Coriolis parameter, $\nu _{t}$ is the eddy viscosity, $\tau _{wi}$ is the wind stress, $\tau _{Si}$ is the wave stresses, and $\tau _{bi}$ is the combined wave-current mean bed shear stress.

Numerical Methods

Temporal Term

The temporal term of the momentum equations is discretized using a first order implicit Euler scheme

$\int \limits _{A}{\frac {\partial (h\phi )}{\partial t}}{\text{d}}A={\frac {\partial }{\partial t}}\int \limits _{A}{(h\phi ){\text{d}}A}={\frac {{{h}^{n+1}}\phi _{}^{n+1}-{{h}^{n}}\phi _{}^{n}}{\Delta t}}\Delta A$

(3)

where $\Delta A$ is the cell area, and $\Delta t$ is the hydrodynamic time step.

Advection Term

The advection scheme obtained using the divergence theorem as where is the outward unit normal on cell face f, is the cell face length and is the total water depth linearly interpolated to the cell face. Here the overbar indicates a cell face interpolation operator described in the following section. For Cartesian grids the cell face unit vector is always aligned with one of the Cartesian coordinates which simplifies the calculation. Defining the cell face normal velocity as the above equation simplifies to

$\int \limits _{A}{\nabla \cdot (h\mathbf {U} \phi )}{\text{d}}A=\oint \limits _{L}{h\phi \left(\mathbf {U} \cdot \mathbf {n} \right)}{\text{d}}L=\sum \limits _{f}^{}{{{\bar {h}}_{f}}\Delta {{l}_{f}}{{\left({{\hat {n}}_{i}}{{U}_{i}}\right)}_{f}}{{\tilde {\phi }}_{f}}}$

(4)

where $\mathbf {n} ={{\hat {n}}_{i}}=({{\hat {n}}_{1}},{{\hat {n}}_{2}})$ is the outward unit normal on cell face f, $\Delta {{l}_{f}}$ is the cell face length and ${{\bar {h}}_{f}}$ is the total water depth linearly interpolated to the cell face. Here the overbar indicates a cell face interpolation operator described in the following section. For Cartesian grids the cell face unit vector is always aligned with one of the Cartesian coordinates which simplifies the calculation. Defining the cell face normal velocity as the above equation simplifies to

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Symbol	Description	Units
$t$	Time	sec
$h$	Total water depth $h=\zeta +\eta$	m
$\zeta$	Still water depth	m
$\eta$	Water surface elevation with respect to the still water elevation	m
$U_{j}$	Current velocity in the jth direction	m/sec
$S$	Sum of Precipitation and evaporation per unit area	m/sec
$g$	Gravitational constant	m/sec2
$\rho$	Water density	kg/m3
$p_{a}$	Atmospheric pressure	Pa
$\nu _{t}$	Turbulent eddy viscosity	m2/sec

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