s_algorithm/text/spatial-discrete.tex

% $Header: /u/gcmpack/mitgcmdoc/part2/spatial-discrete.tex,v 1.1.1.1 2001/08/08 16:15:21 adcroft Exp $
% $Name:  $

\section{Spatial discretization of the dynamical equations}

Spatial discretization is carried out using the finite volume
method. This amounts to a grid-point method (namely second-order
centered finite difference) in the fluid interior but allows
boundaries to intersect a regular grid allowing a more accurate
representation of the position of the boundary. We treat the
horizontal and veritical directions as seperable and thus slightly
differently.

Initialization of grid data is controlled by subroutine {\em
INI\_GRID} which in calls {\em INI\_VERTICAL\_GRID} to initialize the
vertical grid, and then either of {\em INI\_CARTESIAN\_GRID}, {\em
INI\_SPHERICAL\_POLAR\_GRID} or {\em INI\_CURV\-ILINEAR\_GRID} to
initialize the horizontal grid for cartesian, spherical-polar or
curvilinear coordinates respectively.

The reciprocals of all grid quantities are pre-calculated and this is
done in subroutine {\em INI\_MASKS\_ETC} which is called later by
subroutine {\em INITIALIZE\_FIXED}.

All grid descriptors are global arrays and stored in common blocks in
{\em GRID.h} and a generally declared as {\em \_RS}.

\fbox{ \begin{minipage}{4.75in}
{\em S/R INI\_GRID} ({\em model/src/ini\_grid.F})

{\em S/R INI\_MASKS\_ETC} ({\em model/src/ini\_masks\_etc.F})

grid data: ({\em model/inc/GRID.h})
\end{minipage} }


\subsection{The finite volume method: finite volumes versus finite difference}

The finite volume method is used to discretize the equations in
space. The expression ``finite volume'' actually has two meanings; one
involves invocation of the weak formulation (e.g. integral
formulation) and the other involves non-linear expressions for
interpolation of data (e.g. flux limiters). We use both but they can
and will be ddiscussed seperately. The finite volume method discretizes by invoking the weak formulation of the equations or integral form. For example, the 1-D advection-diffusion equation:
\begin{displaymath}
\partial_t \theta + \partial_x ( u \theta - \kappa \partial_x \theta ) = 0
\end{displaymath}
can be discretized by integrating of finite lengths $\Delta x$:
\begin{displaymath}
\Delta x \partial_t \theta + \delta_i ( F ) = 0
\end{displaymath}
is exact but where the flux
\begin{displaymath}
F = u \overline{\theta} - \frac{\kappa}{\Delta x_c} \partial_i \theta
\end{displaymath}
is approximate. The method for obtained $\overline{\theta}$ is
unspecified and non-lienar finite volume methods can be invoked.

....  INCOMPLETE

\subsection{C grid staggering of variables}

\begin{figure}
\centerline{ \resizebox{!}{2in}{ \includegraphics{part2/cgrid3d.eps}} }
\caption{Three dimensional staggering of velocity components. This
facilitates the natural discretization of the continuity and tracer
equations. }
\label{fig:cgrid3d}
\end{figure}

The basic algorithm employed for stepping forward the momentum
equations is based on retaining non-divergence of the flow at all
times. This is most naturally done if the components of flow are
staggered in space in the form of an Arakawa C grid \cite{Arakawa70}.

Fig. \ref{fig:cgrid3d} shows the components of flow ($u$,$v$,$w$)
staggered in space such that the zonal component falls on the
interface between continiuty cells in the zonal direction. Similarly
for the meridional and vertical directions.  The continiuty cell is
synonymous with tracer cells (they are one and the same).


\subsection{Horizontal grid}

\begin{figure}
\centerline{ \begin{tabular}{cc}
  \raisebox{1.5in}{a)}\resizebox{!}{2in}{ \includegraphics{part2/hgrid-Ac.eps}}
& \raisebox{1.5in}{b)}\resizebox{!}{2in}{ \includegraphics{part2/hgrid-Az.eps}}
\\
  \raisebox{1.5in}{c)}\resizebox{!}{2in}{ \includegraphics{part2/hgrid-Au.eps}}
& \raisebox{1.5in}{d)}\resizebox{!}{2in}{ \includegraphics{part2/hgrid-Av.eps}}
\end{tabular} }
\caption{
Staggering of horizontal grid descriptors (lengths and areas). The
grid lines indicate the tracer cell boundaries and are the reference
grid for all panels. a) The area of a tracer cell, $A_c$, is bordered
by the lengths $\Delta x_g$ and $\Delta y_g$. b) The area of a
vorticity cell, $A_\zeta$, is bordered by the lengths $\Delta x_c$ and
$\Delta y_c$. c) The area of a u cell, $A_c$, is bordered by the
lengths $\Delta x_v$ and $\Delta y_f$. d) The area of a v cell, $A_c$,
is bordered by the lengths $\Delta x_f$ and $\Delta y_u$.}
\label{fig:hgrid}
\end{figure}

The model domain is decomposed into tiles and within each tile a
quasi-regular grid is used. A tile is the basic unit of domain
decomposition for parallelization but may be used whether parallized
or not; see section \ref{sect:tiles} for more details. Although the
tiles may be patched together in an unstructured manner
(i.e. irregular or non-tessilating pattern), the interior of tiles is
a structered grid of quadrilateral cells. The horizontal coordinate
system is orthogonal curvilinear meaning we can not necessarily treat
the two horizontal directions as seperable. Instead, each cell in the
horizontal grid is described by the length of it's sides and it's
area.

The grid information is quite general and describes any of the
available coordinates systems, cartesian, spherical-polar or
curvilinear. All that is necessary to distinguish between the
coordinate systems is to initialize the grid data (discriptors)
appropriately.

\marginpar{Caution!}
In the following, we refer to the orientation of quantities on the
computational grid using geographic terminology such as points of the
compass. This is purely for convenience but should note be confused
with the actual geographic orientation of model quantities.

\marginpar{$A_c$: {\bf rAc}}
\marginpar{$\Delta x_g$: {\bf DXg}}
\marginpar{$\Delta y_g$: {\bf DYg}}
Fig.~\ref{fig:hgrid}a shows the tracer cell (synonymous with the
continuity cell). The length of the southern edge, $\Delta x_g$,
western edge, $\Delta y_g$ and surface area, $A_c$, presented in the
vertical are stored in arrays {\bf DXg}, {\bf DYg} and {\bf rAc}. The
``g'' suffix indicates that the lengths are along the defining grid
boundaries. The ``c'' suffix associates the quantity with the cell
centers. The quantities are staggered in space and the indexing is
such that {\bf DXg(i,j)} is positioned to the south of {\bf rAc(i,j)}
and {\bf DYg(i,j)} positioned to the west.

\marginpar{$A_\zeta$: {\bf rAz}}
\marginpar{$\Delta x_c$: {\bf DXc}}
\marginpar{$\Delta y_c$: {\bf DYc}}
Fig.~\ref{fig:hgrid}b shows the vorticity cell. The length of the
southern edge, $\Delta x_c$, western edge, $\Delta y_c$ and surface
area, $A_\zeta$, presented in the vertical are stored in arrays {\bf
DXg}, {\bf DYg} and {\bf rAz}.  The ``z'' suffix indicates that the
lengths are measured between the cell centers and the ``$\zeta$'' suffix
associates points with the vorticity points. The quantities are
staggered in space and the indexing is such that {\bf DXc(i,j)} is
positioned to the north of {\bf rAc(i,j)} and {\bf DYc(i,j)} positioned
to the east.

\marginpar{$A_w$: {\bf rAw}}
\marginpar{$\Delta x_v$: {\bf DXv}}
\marginpar{$\Delta y_f$: {\bf DYf}}
Fig.~\ref{fig:hgrid}c shows the ``u'' or western (w) cell. The length of
the southern edge, $\Delta x_v$, eastern edge, $\Delta y_f$ and
surface area, $A_w$, presented in the vertical are stored in arrays
{\bf DXv}, {\bf DYf} and {\bf rAw}.  The ``v'' suffix indicates that
the length is measured between the v-points, the ``f'' suffix
indicates that the length is measured between the (tracer) cell faces
and the ``w'' suffix associates points with the u-points (w stands for
west). The quantities are staggered in space and the indexing is such
that {\bf DXv(i,j)} is positioned to the south of {\bf rAw(i,j)} and
{\bf DYf(i,j)} positioned to the east.

\marginpar{$A_s$: {\bf rAs}}
\marginpar{$\Delta x_f$: {\bf DXf}}
\marginpar{$\Delta y_u$: {\bf DYu}}
Fig.~\ref{fig:hgrid}d shows the ``v'' or southern (s) cell. The length of
the northern edge, $\Delta x_f$, western edge, $\Delta y_u$ and
surface area, $A_s$, presented in the vertical are stored in arrays
{\bf DXf}, {\bf DYu} and {\bf rAs}.  The ``u'' suffix indicates that
the length is measured between the u-points, the ``f'' suffix
indicates that the length is measured between the (tracer) cell faces
and the ``s'' suffix associates points with the v-points (s stands for
south). The quantities are staggered in space and the indexing is such
that {\bf DXf(i,j)} is positioned to the north of {\bf rAs(i,j)} and
{\bf DYu(i,j)} positioned to the west.

\fbox{ \begin{minipage}{4.75in}
{\em S/R INI\_CARTESIAN\_GRID} ({\em
model/src/ini\_cartesian\_grid.F})

{\em S/R INI\_SPHERICAL\_POLAR\_GRID} ({\em
model/src/ini\_spherical\_polar\_grid.F})

{\em S/R INI\_CURVILINEAR\_GRID} ({\em
model/src/ini\_curvilinear\_grid.F})

$A_c$, $A_\zeta$, $A_w$, $A_s$: {\bf rAc}, {\bf rAz}, {\bf rAw}, {\bf rAs}
({\em GRID.h})

$\Delta x_g$, $\Delta y_g$: {\bf DXg}, {\bf DYg} ({\em GRID.h})

$\Delta x_c$, $\Delta y_c$: {\bf DXc}, {\bf DYc} ({\em GRID.h})

$\Delta x_f$, $\Delta y_f$: {\bf DXf}, {\bf DYf} ({\em GRID.h})

$\Delta x_v$, $\Delta y_u$: {\bf DXv}, {\bf DYu} ({\em GRID.h})

\end{minipage} }

\subsubsection{Reciprocals of horizontal grid descriptors}

%\marginpar{$A_c^{-1}$: {\bf RECIP\_rAc}}
%\marginpar{$A_\zeta^{-1}$: {\bf RECIP\_rAz}}
%\marginpar{$A_w^{-1}$: {\bf RECIP\_rAw}}
%\marginpar{$A_s^{-1}$: {\bf RECIP\_rAs}}
Lengths and areas appear in the denominator of expressions as much as
in the numerator. For efficiency and portability, we pre-calculate the
reciprocal of the horizontal grid quantities so that in-line divisions
can be avoided.

%\marginpar{$\Delta x_g^{-1}$: {\bf RECIP\_DXg}}
%\marginpar{$\Delta y_g^{-1}$: {\bf RECIP\_DYg}}
%\marginpar{$\Delta x_c^{-1}$: {\bf RECIP\_DXc}}
%\marginpar{$\Delta y_c^{-1}$: {\bf RECIP\_DYc}}
%\marginpar{$\Delta x_f^{-1}$: {\bf RECIP\_DXf}}
%\marginpar{$\Delta y_f^{-1}$: {\bf RECIP\_DYf}}
%\marginpar{$\Delta x_v^{-1}$: {\bf RECIP\_DXv}}
%\marginpar{$\Delta y_u^{-1}$: {\bf RECIP\_DYu}}
For each grid descriptor (array) there is a reciprocal named using the
prefix {\bf RECIP\_}. This doubles the amount of storage in {\em
GRID.h} but they are all only 2-D descriptors.

\fbox{ \begin{minipage}{4.75in}
{\em S/R INI\_MASKS\_ETC} ({\em
model/src/ini\_masks\_etc.F})

$A_c^{-1}$: {\bf RECIP\_Ac} ({\em GRID.h})

$A_\zeta^{-1}$: {\bf RECIP\_Az} ({\em GRID.h})

$A_w^{-1}$: {\bf RECIP\_Aw} ({\em GRID.h})

$A_s^{-1}$: {\bf RECIP\_As} ({\em GRID.h})

$\Delta x_g^{-1}$, $\Delta y_g^{-1}$: {\bf RECIP\_DXg}, {\bf RECIP\_DYg} ({\em GRID.h})

$\Delta x_c^{-1}$, $\Delta y_c^{-1}$: {\bf RECIP\_DXc}, {\bf RECIP\_DYc} ({\em GRID.h})

$\Delta x_f^{-1}$, $\Delta y_f^{-1}$: {\bf RECIP\_DXf}, {\bf RECIP\_DYf} ({\em GRID.h})

$\Delta x_v^{-1}$, $\Delta y_u^{-1}$: {\bf RECIP\_DXv}, {\bf RECIP\_DYu} ({\em GRID.h})

\end{minipage} }

\subsubsection{Cartesian coordinates}

Cartesian coordinates are selected when the logical flag {\bf
using\-Cartes\-ianGrid} in namelist {\em PARM04} is set to true. The grid
spacing can be set to uniform via scalars {\bf dXspacing} and {\bf
dYspacing} in namelist {\em PARM04} or to variable resolution by the
vectors {\bf DELX} and {\bf DELY}. Units are normally
meters. Non-dimensional coordinates can be used by interpretting the
gravitational constant as the Rayleigh number.

\subsubsection{Spherical-polar coordinates}

Spherical coordinates are selected when the logical flag {\bf
using\-Spherical\-PolarGrid} in namelist {\em PARM04} is set to true. The
grid spacing can be set to uniform via scalars {\bf dXspacing} and
{\bf dYspacing} in namelist {\em PARM04} or to variable resolution by
the vectors {\bf DELX} and {\bf DELY}. Units of these namelist
variables are alway degrees. The horizontal grid descriptors are
calculated from these namelist variables have units of meters.

\subsubsection{Curvilinear coordinates}

Curvilinear coordinates are selected when the logical flag {\bf
using\-Curvil\-inear\-Grid} in namelist {\em PARM04} is set to true. The
grid spacing can not be set via the namelist. Instead, the grid
descriptors are read from data files, one for each descriptor. As for
other grids, the horizontal grid descriptors have units of meters.


\subsection{Vertical grid}

\begin{figure}
\centerline{ \begin{tabular}{cc}
  \raisebox{4in}{a)} \resizebox{!}{4in}{
  \includegraphics{part2/vgrid-cellcentered.eps}} & \raisebox{4in}{b)}
  \resizebox{!}{4in}{ \includegraphics{part2/vgrid-accurate.eps}}
\end{tabular} }
\caption{Two versions of the vertical grid. a) The cell centered
approach where the interface depths are specified and the tracer
points centered in between the interfaces. b) The interface centered
approach where tracer levels are specified and the w-interfaces are
centered in between.}
\label{fig:vgrid}
\end{figure}

As for the horizontal grid, we use the suffixes ``c'' and ``f'' to
indicates faces and centers. Fig.~\ref{fig:vgrid}a shows the default
vertical grid used by the model.
\marginpar{$\Delta r_f$: {\bf DRf}}
\marginpar{$\Delta r_c$: {\bf DRc}}
$\Delta r_f$ is the difference in $r$
(vertical coordinate) between the faces (i.e. $\Delta r_f \equiv -
\delta_k r$ where the minus sign appears due to the convention that the
surface layer has index $k=1$.).

The vertical grid is calculated in subroutine {\em
INI\_VERTICAL\_GRID} and specified via the vector {\bf DELR} in
namelist {\em PARM04}. The units of ``r'' are either meters or Pascals
depending on the isomorphism being used which in turn is dependent
only on the choise of equation of state.

There are alternative namelist vectors {\bf DELZ} and {\bf DELP} which
dictate whether z- or
\marginpar{Caution!}
p- coordinates are to be used but we intend to
phase this out since they are redundant.

The reciprocals $\Delta r_f^{-1}$ and $\Delta r_c^{-1}$ are
pre-calculated (also in subroutine {\em INI\_VERTICAL\_GRID}). All
vertical grid descriptors are stored in common blocks in {\em GRID.h}.

The above grid (Fig.~\ref{fig:vgrid}a) is known as the cell centered
approach because the tracer points are at cell centers; the cell
centers are mid-way between the cell interfaces. An alternative, the
vertex or interface centered approach, is shown in
Fig.~\ref{fig:vgrid}b. Here, the interior interfaces are positioned
mid-way between the tracer nodes (no longer cell centers). This
approach is formally more accurate for evaluation of hydrostatic
pressure and vertical advection but historically the cell centered
approach has been used. An alternative form of subroutine {\em
INI\_VERTICAL\_GRID} is used to select the interface centered approach
but no run time option is currently available.

\fbox{ \begin{minipage}{4.75in}
{\em S/R INI\_VERTICAL\_GRID} ({\em
model/src/ini\_vertical\_grid.F})

$\Delta r_f$: {\bf DRf} ({\em GRID.h})

$\Delta r_c$: {\bf DRc} ({\em GRID.h})

$\Delta r_f^{-1}$: {\bf RECIP\_DRf} ({\em GRID.h})

$\Delta r_c^{-1}$: {\bf RECIP\_DRc} ({\em GRID.h})

\end{minipage} }


\subsection{Continuity and horizontal pressure gradient terms}

The core algorithm is based on the ``C grid'' discretization of the
continuity equation which can be summarized as:
\begin{eqnarray}
\partial_t u + \frac{1}{\Delta x_c} \delta_i \left. \frac{ \partial \Phi}{\partial r}\right|_{s} \eta + \frac{\epsilon_{nh}}{\Delta x_c} \delta_i \Phi_{nh}' & = & G_u - \frac{1}{\Delta x_c} \delta_i \Phi_h' \\
\partial_t v + \frac{1}{\Delta y_c} \delta_j \left. \frac{ \partial \Phi}{\partial r}\right|_{s} \eta + \frac{\epsilon_{nh}}{\Delta y_c} \delta_j \Phi_{nh}' & = & G_v - \frac{1}{\Delta y_c} \delta_j \Phi_h' \\
\epsilon_{nh} \left( \partial_t w + \frac{1}{\Delta r_c} \delta_k \Phi_{nh}' \right) & = & \epsilon_{nh} G_w + \overline{b}^k - \frac{1}{\Delta r_c} \delta_k \Phi_{h}' \\
\delta_i \Delta y_g \Delta r_f h_w u +
\delta_j \Delta x_g \Delta r_f h_s v +
\delta_k {\cal A}_c w & = & {\cal A}_c \delta_k (P-E)_{r=0}
\label{eq:discrete-continuity}
\end{eqnarray}
where the continuity equation has been most naturally discretized by
staggering the three components of velocity as shown in
Fig.~\ref{fig-cgrid3d}. The grid lengths $\Delta x_c$ and $\Delta y_c$
are the lengths between tracer points (cell centers). The grid lengths
$\Delta x_g$, $\Delta y_g$ are the grid lengths between cell
corners. $\Delta r_f$ and $\Delta r_c$ are the distance (in units of
$r$) between level interfaces (w-level) and level centers (tracer
level). The surface area presented in the vertical is denoted ${\cal
A}_c$.  The factors $h_w$ and $h_s$ are non-dimensional fractions
(between 0 and 1) that represent the fraction cell depth that is
``open'' for fluid flow.
\marginpar{$h_w$: {\bf hFacW}}
\marginpar{$h_s$: {\bf hFacS}}

The last equation, the discrete continuity equation, can be summed in
the vertical to yeild the free-surface equation:
\begin{equation}
{\cal A}_c \partial_t \eta + \delta_i \sum_k \Delta y_g \Delta r_f h_w u + \delta_j \sum_k \Delta x_g \Delta r_f h_s v =
{\cal A}_c(P-E)_{r=0}
\end{equation}
The source term $P-E$ on the rhs of continuity accounts for the local
addition of volume due to excess precipitation and run-off over
evaporation and only enters the top-level of the {\em ocean} model.

\subsection{Hydrostatic balance}

The vertical momentum equation has the hydrostatic or
quasi-hydrostatic balance on the right hand side. This discretization
guarantees that the conversion of potential to kinetic energy as
derived from the buoyancy equation exactly matches the form derived
from the pressure gradient terms when forming the kinetic energy
equation.

In the ocean, using z-ccordinates, the hydrostatic balance terms are
discretized:
\begin{equation}
\epsilon_{nh} \partial_t w
+ g \overline{\rho'}^k + \frac{1}{\Delta z} \delta_k \Phi_h' = \ldots
\end{equation}

In the atmosphere, using p-coordinates, hydrostatic balance is
discretized:
\begin{equation}
\overline{\theta'}^k + \frac{1}{\Delta \Pi} \delta_k \Phi_h' = 0
\end{equation}
where $\Delta \Pi$ is the difference in Exner function between the
pressure points. The non-hydrostatic equations are not available in
the atmosphere.

The difference in approach between ocean and atmosphere occurs because
of the direct use of the ideal gas equation in forming the potential
energy conversion term $\alpha \omega$. The form of these consversion
terms is discussed at length in \cite{Adcroft01}.

Because of the different representation of hydrostatic balance between
ocean and atmosphere there is no elegant way to represent both systems
using an arbitrary coordinate.

The integration for hydrostatic pressure is made in the positive $r$
direction (increasing k-index). For the ocean, this is from the
free-surface down and for the atmosphere this is from the ground up.

The calculations are made in the subroutine {\em
CALC\_PHI\_HYD}. Inside this routine, one of other of the
atmospheric/oceanic form is selected based on the string variable {\bf
buoyancyRelation}.

\subsection{Flux-form momentum equations}

The original finite volume model was based on the Eulerian flux form
momentum equations. This is the default though the vector invariant
form is optionally available (and recommended in some cases).

The ``G's'' (our colloquial name for all terms on rhs!) are broken
into the various advective, Coriolis, horizontal dissipation, vertical
dissipation and metric forces:
\marginpar{$G_u$: {\bf Gu} }
\marginpar{$G_v$: {\bf Gv} }
\marginpar{$G_w$: {\bf Gw} }
\begin{eqnarray}
G_u & = & G_u^{adv} + G_u^{cor} + G_u^{h-diss} + G_u^{v-diss} +
G_u^{metric} + G_u^{nh-metric} \\
G_v & = & G_v^{adv} + G_v^{cor} + G_v^{h-diss} + G_v^{v-diss} +
G_v^{metric} + G_v^{nh-metric} \\
G_w & = & G_w^{adv} + G_w^{cor} + G_w^{h-diss} + G_w^{v-diss} +
G_w^{metric} + G_w^{nh-metric}
\end{eqnarray}
In the hydrostatic limit, $G_w=0$ and $\epsilon_{nh}=0$, reducing the
vertical momentum to hydrostatic balance.

These terms are calculated in routines called from subroutine {\em
CALC\_MOM\_RHS} a collected into the global arrays {\bf Gu}, {\bf Gv},
and {\bf Gw}.

\fbox{ \begin{minipage}{4.75in}
{\em S/R CALC\_MOM\_RHS} ({\em pkg/mom\_fluxform/calc\_mom\_rhs.F})

$G_u$: {\bf Gu} ({\em DYNVARS.h})

$G_v$: {\bf Gv} ({\em DYNVARS.h})

$G_w$: {\bf Gw} ({\em DYNVARS.h})
\end{minipage} }


\subsubsection{Advection of momentum}

The advective operator is second order accurate in space:
\begin{eqnarray}
{\cal A}_w \Delta r_f h_w G_u^{adv} & = &
  \delta_i \overline{ U }^i \overline{ u }^i
+ \delta_j \overline{ V }^i \overline{ u }^j
+ \delta_k \overline{ W }^i \overline{ u }^k \\
{\cal A}_s \Delta r_f h_s G_v^{adv} & = &
  \delta_i \overline{ U }^j \overline{ v }^i
+ \delta_j \overline{ V }^j \overline{ v }^j
+ \delta_k \overline{ W }^j \overline{ v }^k \\
{\cal A}_c \Delta r_c G_w^{adv} & = &
  \delta_i \overline{ U }^k \overline{ w }^i
+ \delta_j \overline{ V }^k \overline{ w }^j
+ \delta_k \overline{ W }^k \overline{ w }^k \\
\end{eqnarray}
and because of the flux form does not contribute to the global budget
of linear momentum. The quantities $U$, $V$ and $W$ are volume fluxes
defined:
\marginpar{$U$: {\bf uTrans} }
\marginpar{$V$: {\bf vTrans} }
\marginpar{$W$: {\bf rTrans} }
\begin{eqnarray}
U & = & \Delta y_g \Delta r_f h_w u \\
V & = & \Delta x_g \Delta r_f h_s v \\
W & = & {\cal A}_c w
\end{eqnarray}
The advection of momentum takes the same form as the advection of
tracers but by a translated advective flow. Consequently, the
conservation of second moments, derived for tracers later, applies to
$u^2$ and $v^2$ and $w^2$ so that advection of momentum correctly
conserves kinetic energy.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_ADV\_UU} ({\em mom\_u\_adv\_uu.F})

{\em S/R MOM\_U\_ADV\_VU} ({\em mom\_u\_adv\_vu.F})

{\em S/R MOM\_U\_ADV\_WU} ({\em mom\_u\_adv\_wu.F})

{\em S/R MOM\_U\_ADV\_UV} ({\em mom\_u\_adv\_uv.F})

{\em S/R MOM\_U\_ADV\_VV} ({\em mom\_u\_adv\_vv.F})

{\em S/R MOM\_U\_ADV\_WV} ({\em mom\_u\_adv\_wv.F})

$uu$, $uv$, $vu$, $vv$: {\bf aF} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Coriolis terms}

The ``pure C grid'' Coriolis terms (i.e. in absence of C-D scheme) are
discretized:
\begin{eqnarray}
{\cal A}_w \Delta r_f h_w G_u^{Cor} & = &
  \overline{ f {\cal A}_c \Delta r_f h_c \overline{ v }^j }^i
- \epsilon_{nh} \overline{ f' {\cal A}_c \Delta r_f h_c \overline{ w }^k }^i \\
{\cal A}_s \Delta r_f h_s G_v^{Cor} & = &
- \overline{ f {\cal A}_c \Delta r_f h_c \overline{ u }^i }^j \\
{\cal A}_c \Delta r_c G_w^{Cor} & = &
 \epsilon_{nh} \overline{ f' {\cal A}_c \Delta r_f h_c \overline{ u }^i }^k
\end{eqnarray}
where the Coriolis parameters $f$ and $f'$ are defined:
\begin{eqnarray}
f & = & 2 \Omega \sin{\phi} \\
f' & = & 2 \Omega \cos{\phi}
\end{eqnarray}
when using spherical geometry, otherwise the $\beta$-plane definition is used:
\begin{eqnarray}
f & = & f_o + \beta y \\
f' & = & 0
\end{eqnarray}

This discretization globally conserves kinetic energy. It should be
noted that despite the use of this discretization in former
publications, all calculations to date have used the following
different discretization:
\begin{eqnarray}
G_u^{Cor} & = &
  f_u \overline{ v }^{ji}
- \epsilon_{nh} f_u' \overline{ w }^{ik} \\
G_v^{Cor} & = &
- f_v \overline{ u }^{ij} \\
G_w^{Cor} & = &
 \epsilon_{nh} f_w' \overline{ u }^{ik}
\end{eqnarray}
\marginpar{Need to change the default in code to match this}
where the subscripts on $f$ and $f'$ indicate evaluation of the
Coriolis parameters at the appropriate points in space. The above
discretization does {\em not} conserve anything, especially energy. An
option to recover this discretization has been retained for backward
compatibility testing (set run-time logical {\bf
useNonconservingCoriolis} to {\em true} which otherwise defaults to
{\em false}).

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_CDSCHEME} ({\em mom\_cdscheme.F})

{\em S/R MOM\_U\_CORIOLIS} ({\em mom\_u\_coriolis.F})

{\em S/R MOM\_V\_CORIOLIS} ({\em mom\_v\_coriolis.F})

$G_u^{Cor}$, $G_v^{Cor}$: {\bf cF} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Curvature metric terms}

The most commonly used coordinate system on the sphere is the
geographic system $(\lambda,\phi)$. The curvilinear nature of these
coordinates on the sphere lead to some ``metric'' terms in the
component momentum equations. Under the thin-atmosphere and
hydrostatic approximations these terms are discretized:
\begin{eqnarray}
{\cal A}_w \Delta r_f h_w G_u^{metric} & = &
  \overline{ \frac{ \overline{u}^i }{a} \tan{\phi} {\cal A}_c \Delta r_f h_c \overline{ v }^j }^i \\
{\cal A}_s \Delta r_f h_s G_v^{metric} & = &
- \overline{ \frac{ \overline{u}^i }{a} \tan{\phi} {\cal A}_c \Delta r_f h_c \overline{ u }^i }^j \\
G_w^{metric} & = & 0
\end{eqnarray}
where $a$ is the radius of the planet (sphericity is assumed) or the
radial distance of the particle (i.e. a function of height).  It is
easy to see that this discretization satisfies all the properties of
the discrete Coriolis terms since the metric factor $\frac{u}{a}
\tan{\phi}$ can be viewed as a modification of the vertical Coriolis
parameter: $f \rightarrow f+\frac{u}{a} \tan{\phi}$.

However, as for the Coriolis terms, a non-energy conserving form has
exclusively been used to date:
\begin{eqnarray}
G_u^{metric} & = & \frac{u \overline{v}^{ij} }{a} \tan{\phi} \\
G_v^{metric} & = & \frac{ \overline{u}^{ij} \overline{u}^{ij}}{a} \tan{\phi}
\end{eqnarray}
where $\tan{\phi}$ is evaluated at the $u$ and $v$ points
respectively.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_METRIC\_SPHERE} ({\em mom\_u\_metric\_sphere.F})

{\em S/R MOM\_V\_METRIC\_SPHERE} ({\em mom\_v\_metric\_sphere.F})

$G_u^{metric}$, $G_v^{metric}$: {\bf mT} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Non-hydrostatic metric terms}

For the non-hydrostatic equations, dropping the thin-atmosphere
approximation re-introduces metric terms involving $w$ and are
required to conserve anglular momentum:
\begin{eqnarray}
{\cal A}_w \Delta r_f h_w G_u^{metric} & = &
- \overline{ \frac{ \overline{u}^i \overline{w}^k }{a} {\cal A}_c \Delta r_f h_c }^i \\
{\cal A}_s \Delta r_f h_s G_v^{metric} & = &
- \overline{ \frac{ \overline{v}^j \overline{w}^k }{a} {\cal A}_c \Delta r_f h_c}^j \\
{\cal A}_c \Delta r_c G_w^{metric} & = &
  \overline{ \frac{ {\overline{u}^i}^2 + {\overline{v}^j}^2}{a} {\cal A}_c \Delta r_f h_c }^k
\end{eqnarray}

Because we are always consistent, even if consistently wrong, we have,
in the past, used a different discretization in the model which is:
\begin{eqnarray}
G_u^{metric} & = &
- \frac{u}{a} \overline{w}^{ik} \\
G_v^{metric} & = &
- \frac{v}{a} \overline{w}^{jk} \\
G_w^{metric} & = &
  \frac{1}{a} ( {\overline{u}^{ik}}^2 + {\overline{v}^{jk}}^2 )
\end{eqnarray}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_METRIC\_NH} ({\em mom\_u\_metric\_nh.F})

{\em S/R MOM\_V\_METRIC\_NH} ({\em mom\_v\_metric\_nh.F})

$G_u^{metric}$, $G_v^{metric}$: {\bf mT} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Lateral dissipation}

Historically, we have represented the SGS Reynolds stresses as simply
down gradient momentum fluxes, ignoring constraints on the stress
tensor such as symmetry.
\begin{eqnarray}
{\cal A}_w \Delta r_f h_w G_u^{h-diss} & = &
  \delta_i  \Delta y_f \Delta r_f h_c \tau_{11}
+ \delta_j  \Delta x_v \Delta r_f h_\zeta \tau_{12} \\
{\cal A}_s \Delta r_f h_s G_v^{h-diss} & = &
  \delta_i  \Delta y_u \Delta r_f h_\zeta \tau_{21}
+ \delta_j  \Delta x_f \Delta r_f h_c \tau_{22}
\end{eqnarray}
\marginpar{Check signs of stress definitions}

The lateral viscous stresses are discretized:
\begin{eqnarray}
\tau_{11} & = & A_h c_{11\Delta}(\phi) \frac{1}{\Delta x_f} \delta_i u
               -A_4 c_{11\Delta^2}(\phi) \frac{1}{\Delta x_f} \delta_i \nabla^2 u \\
\tau_{12} & = & A_h c_{12\Delta}(\phi) \frac{1}{\Delta y_u} \delta_j u
               -A_4 c_{12\Delta^2}(\phi)\frac{1}{\Delta y_u} \delta_j \nabla^2 u \\
\tau_{21} & = & A_h c_{21\Delta}(\phi) \frac{1}{\Delta x_v} \delta_i v
               -A_4 c_{21\Delta^2}(\phi) \frac{1}{\Delta x_v} \delta_i \nabla^2 v \\
\tau_{22} & = & A_h c_{22\Delta}(\phi) \frac{1}{\Delta y_f} \delta_j v
               -A_4 c_{22\Delta^2}(\phi) \frac{1}{\Delta y_f} \delta_j \nabla^2 v
\end{eqnarray}
where the non-dimensional factors $c_{lm\Delta^n}(\phi), \{l,m,n\} \in
\{1,2\}$ define the ``cosine'' scaling with latitude which can be
applied in various ad-hoc ways. For instance, $c_{11\Delta} =
c_{21\Delta} = (\cos{\phi})^{3/2}$, $c_{12\Delta}=c_{22\Delta}=0$ would
represent the an-isotropic cosine scaling typically used on the
``lat-lon'' grid for Laplacian viscosity.
\marginpar{Need to tidy up method for controlling this in code}

It should be noted that dispite the ad-hoc nature of the scaling, some
scaling must be done since on a lat-lon grid the converging meridians
make it very unlikely that a stable viscosity parameter exists across
the entire model domain.

The Laplacian viscosity coefficient, $A_h$ ({\bf viscAh}), has units
of $m^2 s^{-1}$. The bi-harmonic viscosity coefficient, $A_4$ ({\bf
viscA4}), has units of $m^4 s^{-1}$.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_XVISCFLUX} ({\em mom\_u\_xviscflux.F})

{\em S/R MOM\_U\_YVISCFLUX} ({\em mom\_u\_yviscflux.F})

{\em S/R MOM\_V\_XVISCFLUX} ({\em mom\_v\_xviscflux.F})

{\em S/R MOM\_V\_YVISCFLUX} ({\em mom\_v\_yviscflux.F})

$\tau_{11}$, $\tau_{12}$, $\tau_{22}$, $\tau_{22}$: {\bf vF}, {\bf
v4F} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }

Two types of lateral boundary condition exist for the lateral viscous
terms, no-slip and free-slip.

The free-slip condition is most convenient to code since it is
equivalent to zero-stress on boundaries. Simple masking of the stress
components sets them to zero. The fractional open stress is properly
handled using the lopped cells.

The no-slip condition defines the normal gradient of a tangential flow
such that the flow is zero on the boundary. Rather than modify the
stresses by using complicated functions of the masks and ``ghost''
points (see \cite{Adcroft+Marshall98}) we add the boundary stresses as
an additional source term in cells next to solid boundaries. This has
the advantage of being able to cope with ``thin walls'' and also makes
the interior stress calculation (code) independent of the boundary
conditions. The ``body'' force takes the form:
\begin{eqnarray}
G_u^{side-drag} & = &
\frac{4}{\Delta z_f} \overline{ (1-h_\zeta) \frac{\Delta x_v}{\Delta y_u} }^j
\left( A_h c_{12\Delta}(\phi) u - A_4 c_{12\Delta^2}(\phi) \nabla^2 u \right)
\\
G_v^{side-drag} & = &
\frac{4}{\Delta z_f} \overline{ (1-h_\zeta) \frac{\Delta y_u}{\Delta x_v} }^i
\left( A_h c_{21\Delta}(\phi) v - A_4 c_{21\Delta^2}(\phi) \nabla^2 v \right)
\end{eqnarray}

In fact, the above discretization is not quite complete because it
assumes that the bathymetry at velocity points is deeper than at
neighbouring vorticity points, e.g. $1-h_w < 1-h_\zeta$

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_SIDEDRAG} ({\em mom\_u\_sidedrag.F})

{\em S/R MOM\_V\_SIDEDRAG} ({\em mom\_v\_sidedrag.F})

$G_u^{side-drag}$, $G_v^{side-drag}$: {\bf vF} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Vertical dissipation}

Vertical viscosity terms are discretized with only partial adherence
to the variable grid lengths introduced by the finite volume
formulation. This reduces the formal accuracy of these terms to just
first order but only next to boundaries; exactly where other terms
appear such as linar and quadratic bottom drag.
\begin{eqnarray}
G_u^{v-diss} & = &
\frac{1}{\Delta r_f h_w} \delta_k \tau_{13} \\
G_v^{v-diss} & = &
\frac{1}{\Delta r_f h_s} \delta_k \tau_{23} \\
G_w^{v-diss} & = & \epsilon_{nh}
\frac{1}{\Delta r_f h_d} \delta_k \tau_{33}
\end{eqnarray}
represents the general discrete form of the vertical dissipation terms.

In the interior the vertical stresses are discretized:
\begin{eqnarray}
\tau_{13} & = & A_v \frac{1}{\Delta r_c} \delta_k u \\
\tau_{23} & = & A_v \frac{1}{\Delta r_c} \delta_k v \\
\tau_{33} & = & A_v \frac{1}{\Delta r_f} \delta_k w
\end{eqnarray}
It should be noted that in the non-hydrostatic form, the stress tensor
is even less consistent than for the hydrostatic (see Wazjowicz
\cite{Waojz}). It is well known how to do this properly (see Griffies
\cite{Griffies}) and is on the list of to-do's.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_RVISCLFUX} ({\em mom\_u\_rviscflux.F})

{\em S/R MOM\_V\_RVISCLFUX} ({\em mom\_v\_rviscflux.F})

$\tau_{13}$: {\bf urf} (local to {\em calc\_mom\_rhs.F})

$\tau_{23}$: {\bf vrf} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


As for the lateral viscous terms, the free-slip condition is
equivalent to simply setting the stress to zero on boundaries.  The
no-slip condition is implemented as an additional term acting on top
of the interior and free-slip stresses. Bottom drag represents
additional friction, in addition to that imposed by the no-slip
condition at the bottom. The drag is cast as a stress expressed as a
linear or quadratic function of the mean flow in the layer above the
topography:
\begin{eqnarray}
\tau_{13}^{bottom-drag} & = &
\left(
2 A_v \frac{1}{\Delta r_c}
+ r_b
+ C_d \sqrt{ \overline{2 KE}^i }
\right) u \\
\tau_{23}^{bottom-drag} & = &
\left(
2 A_v \frac{1}{\Delta r_c}
+ r_b
+ C_d \sqrt{ \overline{2 KE}^j }
\right) v
\end{eqnarray}
where these terms are only evaluated immediately above topography.
$r_b$ ({\bf bottomDragLinear}) has units of $m s^{-1}$ and a typical value
of the order 0.0002 $m s^{-1}$. $C_d$ ({\bf bottomDragQuadratic}) is
dimensionless with typical values in the range 0.001--0.003.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_BOTTOMDRAG} ({\em mom\_u\_bottomdrag.F})

{\em S/R MOM\_V\_BOTTOMDRAG} ({\em mom\_v\_bottomdrag.F})

$\tau_{13}^{bottom-drag}$, $\tau_{23}^{bottom-drag}$: {\bf vf} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsection{Tracer equations}

The tracer equations are discretized consistantly with the continuity
equation to facilitate conservation properties analogous to the
continuum:
\begin{equation}
{\cal A}_c \Delta r_f h_c \partial_\theta
+ \delta_i U \overline{ \theta }^i
+ \delta_j V \overline{ \theta }^j
+ \delta_k W \overline{ \theta }^k
= {\cal A}_c \Delta r_f h_c {\cal S}_\theta + \theta {\cal A}_c \delta_k (P-E)_{r=0}
\end{equation}
The quantities $U$, $V$ and $W$ are volume fluxes defined:
\marginpar{$U$: {\bf uTrans} }
\marginpar{$V$: {\bf vTrans} }
\marginpar{$W$: {\bf rTrans} }
\begin{eqnarray}
U & = & \Delta y_g \Delta r_f h_w u \\
V & = & \Delta x_g \Delta r_f h_s v \\
W & = & {\cal A}_c w
\end{eqnarray}
${\cal S}$ represents the ``parameterized'' SGS processes and
physics associated with the tracer. For instance, potential
temperature equation in the ocean has is forced by surface and
partially penetrating heat fluxes:
\begin{equation}
{\cal A}_c \Delta r_f h_c {\cal S}_\theta = \frac{1}{c_p \rho_o} \delta_k {\cal A}_c {\cal Q}
\end{equation}
while the salt equation has no real sources, ${\cal S}=0$, which
leaves just the $P-E$ term.

The continuity equation can be recovered by setting ${\cal Q}=0$ and
$\theta=1$. The term $\theta (P-E)_{r=0}$ is required to retain local
conservation of $\theta$. Global conservation is not possible using
the flux-form (as here) and a linearized free-surface
(\cite{Griffies00,Campin02}).


\subsection{Derivation of discrete energy conservation}

These discrete equations conserve kinetic plus potential energy using the
following definitions:
\begin{equation}
KE = \frac{1}{2} \left( \overline{ u^2 }^i + \overline{ v^2 }^j +
\epsilon_{nh} \overline{ w^2 }^k \right)
\end{equation}


\subsection{Vector invariant momentum equations}

The finite volume method lends itself to describing the continuity and
tracer equations in curvilinear coordinate systems but the appearance
of new metric terms in the flux-form momentum equations makes
generalizing them far from elegant. The vector invariant form of the
momentum equations are exactly that; invariant under coordinate
transformations.

The non-hydrostatic vector invariant equations read:
\begin{equation}
\partial_t \vec{v} + ( 2\vec{\Omega} + \vec{\zeta}) \wedge \vec{v}
- b \hat{r}
+ \vec{\nabla} B = \vec{\nabla} \cdot \vec{\bf \tau}
\end{equation}
which describe motions in any orthogonal curvilinear coordinate
system. Here, $B$ is the Bernoulli function and $\vec{\zeta}=\nabla
\wedge \vec{v}$ is the vorticity vector. We can take advantage of the
elegance of these equations when discretizing them and use the
discrete definitions of the grad, curl and divergence operators to
satisfy constraints. We can also consider the analogy to forming
derived equations, such as the vorticity equation, and examine how the
discretization can be adjusted to give suitable vorticity advection
among other things.

The underlying algorithm is the same as for the flux form
equations. All that has changed is the contents of the ``G's''. For
the time-being, only the hydrostatic terms have been coded but we will
indicate the points where non-hydrostatic contributions will enter:
\begin{eqnarray}
G_u & = & G_u^{fv} + G_u^{\zeta_3 v} + G_u^{\zeta_2 w} + G_u^{\partial_x B}
+ G_u^{\partial_z \tau^x} + G_u^{h-dissip} + G_u^{v-dissip} \\
G_v & = & G_v^{fu} + G_v^{\zeta_3 u} + G_v^{\zeta_1 w} + G_v^{\partial_y B}
+ G_v^{\partial_z \tau^y} + G_v^{h-dissip} + G_v^{v-dissip} \\
G_w & = & G_w^{fu} + G_w^{\zeta_1 v} + G_w^{\zeta_2 u} + G_w^{\partial_z B}
+ G_w^{h-dissip} + G_w^{v-dissip}
\end{eqnarray}

\fbox{ \begin{minipage}{4.75in}
{\em S/R CALC\_MOM\_RHS} ({\em pkg/mom\_vecinv/calc\_mom\_rhs.F})

$G_u$: {\bf Gu} ({\em DYNVARS.h})

$G_v$: {\bf Gv} ({\em DYNVARS.h})

$G_w$: {\bf Gw} ({\em DYNVARS.h})
\end{minipage} }

\subsubsection{Relative vorticity}

The vertical component of relative vorticity is explicitly calculated
and use in the discretization. The particular form is crucial for
numerical stablility; alternative definitions break the conservation
properties of the discrete equations.

Relative vorticity is defined:
\begin{equation}
\zeta_3 = \frac{\Gamma}{A_\zeta}
= \frac{1}{{\cal A}_\zeta} ( \delta_i \Delta y_c v - \delta_j \Delta x_c u )
\end{equation}
where ${\cal A}_\zeta$ is the area of the vorticity cell presented in
the vertical and $\Gamma$ is the circulation about that cell.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_CALC\_RELVORT3} ({\em mom\_vi\_calc\_relvort3.F})

$\zeta_3$: {\bf vort3} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Kinetic energy}

The kinetic energy, denoted $KE$, is defined:
\begin{equation}
KE = \frac{1}{2} ( \overline{ u^2 }^i + \overline{ v^2 }^j 
+ \epsilon_{nh} \overline{ w^2 }^k )
\end{equation}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_CALC\_KE} ({\em mom\_vi\_calc\_ke.F})

$KE$: {\bf KE} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Coriolis terms}

The potential enstrophy conserving form of the linear Coriolis terms
are written:
\begin{eqnarray}
G_u^{fv} & = &
\frac{1}{\Delta x_c}
\overline{ \frac{f}{h_\zeta} }^j \overline{ \overline{ \Delta x_g h_s v }^j }^i \\
G_v^{fu} & = & -
\frac{1}{\Delta y_c}
\overline{ \frac{f}{h_\zeta} }^i \overline{ \overline{ \Delta y_g h_w u }^i }^j
\end{eqnarray}
Here, the Coriolis parameter $f$ is defined at vorticity (corner)
points.
\marginpar{$f$: {\bf fCoriG}}
\marginpar{$h_\zeta$: {\bf hFacZ}}

The potential enstrophy conserving form of the non-linear Coriolis
terms are written:
\begin{eqnarray}
G_u^{\zeta_3 v} & = &
\frac{1}{\Delta x_c}
\overline{ \frac{\zeta_3}{h_\zeta} }^j \overline{ \overline{ \Delta x_g h_s v }^j }^i \\
G_v^{\zeta_3 u} & = & -
\frac{1}{\Delta y_c}
\overline{ \frac{\zeta_3}{h_\zeta} }^i \overline{ \overline{ \Delta y_g h_w u }^i }^j
\end{eqnarray}
\marginpar{$\zeta_3$: {\bf vort3}}

The Coriolis terms can also be evaluated together and expressed in
terms of absolute vorticity $f+\zeta_3$. The potential enstrophy
conserving form using the absolute vorticity is written:
\begin{eqnarray}
G_u^{fv} + G_u^{\zeta_3 v} & = &
\frac{1}{\Delta x_c}
\overline{ \frac{f + \zeta_3}{h_\zeta} }^j \overline{ \overline{ \Delta x_g h_s v }^j }^i \\
G_v^{fu} + G_v^{\zeta_3 u} & = & -
\frac{1}{\Delta y_c}
\overline{ \frac{f + \zeta_3}{h_\zeta} }^i \overline{ \overline{ \Delta y_g h_w u }^i }^j
\end{eqnarray}

\marginpar{Run-time control needs to be added for these options} The
disctinction between using absolute vorticity or relative vorticity is
useful when constructing higher order advection schemes; monotone
advection of relative vorticity behaves differently to monotone
advection of absolute vorticity. Currently the choice of
relative/absolute vorticity, centered/upwind/high order advection is
available only through commented subroutine calls.

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_CORIOLIS} ({\em mom\_vi\_coriolis.F})

{\em S/R MOM\_VI\_U\_CORIOLIS} ({\em mom\_vi\_u\_coriolis.F})

{\em S/R MOM\_VI\_V\_CORIOLIS} ({\em mom\_vi\_v\_coriolis.F})

$G_u^{fv}$, $G_u^{\zeta_3 v}$: {\bf uCf} (local to {\em calc\_mom\_rhs.F})

$G_v^{fu}$, $G_v^{\zeta_3 u}$: {\bf vCf} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Shear terms}

The shear terms ($\zeta_2w$ and $\zeta_1w$) are are discretized to
guarantee that no spurious generation of kinetic energy is possible;
the horizontal gradient of Bernoulli function has to be consistent
with the vertical advection of shear:
\marginpar{N-H terms have not been tried!}
\begin{eqnarray}
G_u^{\zeta_2 w} & = &
\frac{1}{ {\cal A}_w \Delta r_f h_w } \overline{
\overline{ {\cal A}_c w }^i ( \delta_k u - \epsilon_{nh} \delta_j w )
}^k \\
G_v^{\zeta_1 w} & = &
\frac{1}{ {\cal A}_s \Delta r_f h_s } \overline{
\overline{ {\cal A}_c w }^i ( \delta_k u - \epsilon_{nh} \delta_j w )
}^k
\end{eqnarray}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_U\_VERTSHEAR} ({\em mom\_vi\_u\_vertshear.F})

{\em S/R MOM\_VI\_V\_VERTSHEAR} ({\em mom\_vi\_v\_vertshear.F})

$G_u^{\zeta_2 w}$: {\bf uCf} (local to {\em calc\_mom\_rhs.F})

$G_v^{\zeta_1 w}$: {\bf vCf} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Gradient of Bernoulli function}

\begin{eqnarray}
G_u^{\partial_x B} & = &
\frac{1}{\Delta x_c} \delta_i ( \phi' + KE ) \\
G_v^{\partial_y B} & = &
\frac{1}{\Delta x_y} \delta_j ( \phi' + KE )
%G_w^{\partial_z B} & = &
%\frac{1}{\Delta r_c} h_c \delta_k ( \phi' + KE )
\end{eqnarray}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_U\_GRAD\_KE} ({\em mom\_vi\_u\_grad\_ke.F})

{\em S/R MOM\_VI\_V\_GRAD\_KE} ({\em mom\_vi\_v\_grad\_ke.F})

$G_u^{\partial_x KE}$: {\bf uCf} (local to {\em calc\_mom\_rhs.F})

$G_v^{\partial_y KE}$: {\bf vCf} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Horizontal dissipation}

The horizontal divergence, a complimentary quantity to relative
vorticity, is used in parameterizing the Reynolds stresses and is
discretized:
\begin{equation}
D = \frac{1}{{\cal A}_c h_c} (
  \delta_i \Delta y_g h_w u
+ \delta_j \Delta x_g h_s v )
\end{equation}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_CALC\_HDIV} ({\em mom\_vi\_calc\_hdiv.F})

$D$: {\bf hDiv} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Horizontal dissipation}

The following discretization of horizontal dissipation conserves
potential vorticity (thickness weighted relative vorticity) and
divergence and dissipates energy, enstrophy and divergence squared:
\begin{eqnarray}
G_u^{h-dissip} & = &
  \frac{1}{\Delta x_c} \delta_i ( A_D D - A_{D4} D^*)
- \frac{1}{\Delta y_u h_w} \delta_j h_\zeta ( A_\zeta \zeta - A_{\zeta4} \zeta^* )
\\
G_v^{h-dissip} & = &
  \frac{1}{\Delta x_v h_s} \delta_i h_\zeta ( A_\zeta \zeta - A_\zeta \zeta^* )
+ \frac{1}{\Delta y_c} \delta_j ( A_D D - A_{D4} D^* )
\end{eqnarray}
where
\begin{eqnarray}
D^* & = & \frac{1}{{\cal A}_c h_c} (
  \delta_i \Delta y_g h_w \nabla^2 u
+ \delta_j \Delta x_g h_s \nabla^2 v ) \\
\zeta^* & = & \frac{1}{{\cal A}_\zeta} (
  \delta_i \Delta y_c \nabla^2 v
- \delta_j \Delta x_c \nabla^2 u )
\end{eqnarray}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_VI\_HDISSIP} ({\em mom\_vi\_hdissip.F})

$G_u^{h-dissip}$: {\bf uDiss} (local to {\em calc\_mom\_rhs.F})

$G_v^{h-dissip}$: {\bf vDiss} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }


\subsubsection{Vertical dissipation}

Currently, this is exactly the same code as the flux form equations.
\begin{eqnarray}
G_u^{v-diss} & = &
\frac{1}{\Delta r_f h_w} \delta_k \tau_{13} \\
G_v^{v-diss} & = &
\frac{1}{\Delta r_f h_s} \delta_k \tau_{23}
\end{eqnarray}
represents the general discrete form of the vertical dissipation terms.

In the interior the vertical stresses are discretized:
\begin{eqnarray}
\tau_{13} & = & A_v \frac{1}{\Delta r_c} \delta_k u \\
\tau_{23} & = & A_v \frac{1}{\Delta r_c} \delta_k v
\end{eqnarray}

\fbox{ \begin{minipage}{4.75in}
{\em S/R MOM\_U\_RVISCLFUX} ({\em mom\_u\_rviscflux.F})

{\em S/R MOM\_V\_RVISCLFUX} ({\em mom\_v\_rviscflux.F})

$\tau_{13}$: {\bf urf} (local to {\em calc\_mom\_rhs.F})

$\tau_{23}$: {\bf vrf} (local to {\em calc\_mom\_rhs.F})
\end{minipage} }