--- manual/s_algorithm/text/spatial-discrete.tex 2001/10/24 15:21:27 1.9 +++ manual/s_algorithm/text/spatial-discrete.tex 2001/11/13 18:15:26 1.11 @@ -1,4 +1,4 @@ -% $Header: /home/ubuntu/mnt/e9_copy/manual/s_algorithm/text/spatial-discrete.tex,v 1.9 2001/10/24 15:21:27 cnh Exp $ +% $Header: /home/ubuntu/mnt/e9_copy/manual/s_algorithm/text/spatial-discrete.tex,v 1.11 2001/11/13 18:15:26 adcroft Exp $ % $Name: $ \section{Spatial discretization of the dynamical equations} @@ -8,7 +8,7 @@ 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 differently. +horizontal and vertical directions as separable and differently. \input{part2/notation} @@ -37,7 +37,7 @@ \begin{displaymath} \Delta x \partial_t \theta + \delta_i ( F ) = 0 \end{displaymath} -is exact if $\theta(x)$ is peice-wise constant over the interval +is exact if $\theta(x)$ is piece-wise constant over the interval $\Delta x_i$ or more generally if $\theta_i$ is defined as the average over the interval $\Delta x_i$. @@ -57,12 +57,12 @@ interior of a fluid. Differences arise at boundaries where a boundary is not positioned on a regular or smoothly varying grid. This method is used to represent the topography using lopped cell, see -\cite{Adcroft98}. Subtle difference also appear in more than one +\cite{adcroft:97}. Subtle difference also appear in more than one dimension away from boundaries. This happens because the each -direction is discretized independantly in the finite difference method +direction is discretized independently in the finite difference method while the integrating over finite volume implicitly treats all directions simultaneously. Illustration of this is given in -\cite{Adcroft02}. +\cite{ac:02}. \subsection{C grid staggering of variables} @@ -79,12 +79,12 @@ 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}. +staggered in space in the form of an Arakawa C grid \cite{arakawa:77}. 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 +interface between continuity cells in the zonal direction. Similarly +for the meridional and vertical directions. The continuity cell is synonymous with tracer cells (they are one and the same). @@ -141,20 +141,20 @@ 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 +decomposition for parallelization but may be used whether parallelized 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 +a structured 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 +the two horizontal directions as separable. 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) +coordinate systems is to initialize the grid data (descriptors) appropriately. In the following, we refer to the orientation of quantities on the @@ -293,7 +293,7 @@ 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 +meters. Non-dimensional coordinates can be used by interpreting the gravitational constant as the Rayleigh number. \subsubsection{Spherical-polar coordinates} @@ -347,7 +347,7 @@ 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. +only on the choice of equation of state. There are alternative namelist vectors {\bf DELZ} and {\bf DELP} which dictate whether z- or @@ -400,13 +400,13 @@ \label{fig:hfacs} \end{figure} -\cite{Adcroft97} presented two alternatives to the step-wise finite +\cite{adcroft:97} presented two alternatives to the step-wise finite difference representation of topography. The method is known to the engineering community as {\em intersecting boundary method}. It involves allowing the boundary to intersect a grid of cells thereby modifying the shape of those cells intersected. We suggested allowing -the topgoraphy to take on a peice-wise linear representation (shaved -cells) or a simpler piecewise constant representaion (partial step). +the topography to take on a piece-wise linear representation (shaved +cells) or a simpler piecewise constant representation (partial step). Both show dramatic improvements in solution compared to the traditional full step representation, the piece-wise linear being the best. However, the storage requirements are excessive so the simpler @@ -420,7 +420,7 @@ \marginpar{$h_s$: {\bf hFacS}} The physical thickness of a tracer cell is given by $h_c(i,j,k) \Delta r_f(k)$ and the physical thickness of the open side is given by -$h_w(i,j,k) \Delta r_f(k)$. Three 3-D discriptors $h_c$, $h_w$ and +$h_w(i,j,k) \Delta r_f(k)$. Three 3-D descriptors $h_c$, $h_w$ and $h_s$ are used to describe the geometry: {\bf hFacC}, {\bf hFacW} and {\bf hFacS} respectively. These are calculated in subroutine {\em INI\_MASKS\_ETC} along with there reciprocals {\bf RECIP\_hFacC}, {\bf @@ -484,7 +484,7 @@ \marginpar{$h_s$: {\bf hFacS}} The last equation, the discrete continuity equation, can be summed in -the vertical to yeild the free-surface equation: +the vertical to yield 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 @@ -503,7 +503,7 @@ from the pressure gradient terms when forming the kinetic energy equation. -In the ocean, using z-ccordinates, the hydrostatic balance terms are +In the ocean, using z-coordinates, the hydrostatic balance terms are discretized: \begin{equation} \epsilon_{nh} \partial_t w @@ -523,8 +523,8 @@ 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}. +energy conversion term $\alpha \omega$. The form of these conversion +terms is discussed at length in \cite{adcroft:02}. Because of the different representation of hydrostatic balance between ocean and atmosphere there is no elegant way to represent both systems