--- manual/s_overview/text/manual.tex	2001/11/13 20:13:07	1.9
+++ manual/s_overview/text/manual.tex	2001/11/19 19:58:20	1.13
@@ -1,4 +1,4 @@
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 %tci%\documentclass[12pt]{book}
@@ -34,7 +34,7 @@
 
 % Section: Overview
 
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 \section{Introduction}
@@ -83,13 +83,57 @@
 computational platforms.
 \end{itemize}
 
-Key publications reporting on and charting the development of the model are
-listed in an Appendix.
+Key publications reporting on and charting the development of the model are:
+
+\begin{verbatim}
+
+Hill, C. and J. Marshall, (1995)
+Application of a Parallel Navier-Stokes Model to Ocean Circulation in 
+Parallel Computational Fluid Dynamics
+In Proceedings of Parallel Computational Fluid Dynamics: Implementations 
+and Results Using Parallel Computers, 545-552.
+Elsevier Science B.V.: New York
+
+Marshall, J., C. Hill, L. Perelman, and A. Adcroft, (1997)
+Hydrostatic, quasi-hydrostatic, and nonhydrostatic ocean modeling,
+J. Geophysical Res., 102(C3), 5733-5752.
+
+Marshall, J., A. Adcroft, C. Hill, L. Perelman, and C. Heisey, (1997)
+A finite-volume, incompressible Navier Stokes model for studies of the ocean
+on parallel computers,
+J. Geophysical Res., 102(C3), 5753-5766.
+
+Adcroft, A.J., Hill, C.N. and J. Marshall, (1997)
+Representation of topography by shaved cells in a height coordinate ocean
+model
+Mon Wea Rev, vol 125, 2293-2315
+
+Marshall, J., Jones, H. and C. Hill, (1998)
+Efficient ocean modeling using non-hydrostatic algorithms
+Journal of Marine Systems, 18, 115-134
+
+Adcroft, A., Hill C. and J. Marshall: (1999)
+A new treatment of the Coriolis terms in C-grid models at both high and low
+resolutions,
+Mon. Wea. Rev. Vol 127, pages 1928-1936
+
+Hill, C, Adcroft,A., Jamous,D., and J. Marshall, (1999)
+A Strategy for Terascale Climate Modeling.
+In Proceedings of the Eight ECMWF Workshop on the Use of Parallel Processors
+in Meteorology
+
+Marotzke, J, Giering,R., Zhang, K.Q., Stammer,D., Hill,C., and T.Lee, (1999)
+Construction of the adjoint MIT ocean general circulation model and 
+application to Atlantic heat transport variability
+J. Geophysical Res., 104(C12), 29,529-29,547.
+
+
+\end{verbatim}
 
 We begin by briefly showing some of the results of the model in action to
 give a feel for the wide range of problems that can be addressed using it.
 
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 \section{Illustrations of the model in action}
@@ -102,7 +146,7 @@
 numerical algorithm and implementation that lie behind these calculations is
 given later. Indeed many of the illustrative examples shown below can be
 easily reproduced: simply download the model (the minimum you need is a PC
-running linux, together with a FORTRAN\ 77 compiler) and follow the examples
+running Linux, together with a FORTRAN\ 77 compiler) and follow the examples
 described in detail in the documentation.
 
 \subsection{Global atmosphere: `Held-Suarez' benchmark}
@@ -126,7 +170,7 @@
 %% CNHend
 
 As described in Adcroft (2001), a `cubed sphere' is used to discretize the
-globe permitting a uniform gridding and obviated the need to Fourier filter.
+globe permitting a uniform griding and obviated the need to Fourier filter.
 The `vector-invariant' form of MITgcm supports any orthogonal curvilinear
 grid, of which the cubed sphere is just one of many choices.
 
@@ -163,7 +207,7 @@
 visible.
 
 %% CNHbegin
-\input{part1/ocean_gyres_figure}
+\input{part1/atl6_figure}
 %% CNHend
 
 
@@ -231,7 +275,7 @@
 
 As one example of application of the MITgcm adjoint, Figure \ref{fig:hf-sensitivity}
 maps the gradient $\frac{\partial J}{\partial \mathcal{H}}$where $J$ is the magnitude
-of the overturning streamfunction shown in figure \ref{fig:large-scale-circ}
+of the overturning stream-function shown in figure \ref{fig:large-scale-circ}
 at 60$^{\circ }$N and $
 \mathcal{H}(\lambda,\varphi)$ is the mean, local air-sea heat flux over
 a 100 year period. We see that $J$ is
@@ -248,7 +292,7 @@
 An important application of MITgcm is in state estimation of the global
 ocean circulation. An appropriately defined `cost function', which measures
 the departure of the model from observations (both remotely sensed and
-insitu) over an interval of time, is minimized by adjusting `control
+in-situ) over an interval of time, is minimized by adjusting `control
 parameters' such as air-sea fluxes, the wind field, the initial conditions
 etc. Figure \ref{fig:assimilated-globes} shows an estimate of the time-mean
 surface elevation of the ocean obtained by bringing the model in to
@@ -256,7 +300,7 @@
 1992-1997. {\bf CHANGE THIS TEXT - FIG FROM PATRICK/CARL/DETLEF}
 
 %% CNHbegin
-\input{part1/globes_figure}
+\input{part1/assim_figure}
 %% CNHend
 
 \subsection{Ocean biogeochemical cycles}
@@ -277,7 +321,7 @@
 \subsection{Simulations of laboratory experiments}
 
 Figure \ref{fig:lab-simulation} shows MITgcm being used to simulate a 
-laboratory experiment enquiring in to the dynamics of the Antarctic Circumpolar Current (ACC). An
+laboratory experiment inquiring in to the dynamics of the Antarctic Circumpolar Current (ACC). An
 initially homogeneous tank of water ($1m$ in diameter) is driven from its
 free surface by a rotating heated disk. The combined action of mechanical
 and thermal forcing creates a lens of fluid which becomes baroclinically
@@ -289,7 +333,7 @@
 \input{part1/lab_figure}
 %%CNHend
 
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 \section{Continuous equations in `r' coordinates}
@@ -432,7 +476,7 @@
 
 \begin{equation}
 \dot{r}=\frac{Dr}{Dt}atr=R_{moving}\text{ \
-(oceansurface,bottomoftheatmosphere)}  \label{eq:movingbc}
+(ocean surface,bottom of the atmosphere)}  \label{eq:movingbc}
 \end{equation}
 
 Here
@@ -1028,7 +1072,7 @@
 Tangent linear and adjoint counterparts of the forward model are described
 in Chapter 5.
 
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 \section{Appendix ATMOSPHERE}
@@ -1155,7 +1199,7 @@
 \frac{D\theta }{Dt} &=&\frac{\mathcal{Q}}{\Pi } 
 \end{eqnarray}
 
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 \section{Appendix OCEAN}
@@ -1178,7 +1222,7 @@
 \label{eq:non-boussinesq}
 \end{eqnarray}
 These equations permit acoustics modes, inertia-gravity waves,
-non-hydrostatic motions, a geostrophic (Rossby) mode and a thermo-haline
+non-hydrostatic motions, a geostrophic (Rossby) mode and a thermohaline
 mode. As written, they cannot be integrated forward consistently - if we
 step $\rho $ forward in (\ref{eq-zns-cont}), the answer will not be
 consistent with that obtained by stepping (\ref{eq-zns-heat}) and (\ref
@@ -1371,7 +1415,7 @@
 _{nh}=0$ form of these equations that are used throughout the ocean modeling
 community and referred to as the primitive equations (HPE).
 
-% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.9 2001/11/13 20:13:07 adcroft Exp $
+% $Header: /home/ubuntu/mnt/e9_copy/manual/s_overview/text/manual.tex,v 1.13 2001/11/19 19:58:20 cnh Exp $
 % $Name:  $
 
 \section{Appendix:OPERATORS}