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-revision 1.9 by molod,
Mon Jul 18 20:45:27 2005 UTC
+revision 1.16 by edhill,
Wed Jun 28 15:12:14 2006 UTC
 Line 8
  \subsubsection{Introduction}
  The fizhi (high-end atmospheric physics) package includes a collection of state-of-the-art
  physical parameterizations for atmospheric radiation, cumulus convection, atmospheric
- boundary layer turbulence, and land surface processes.
+ boundary layer turbulence, and land surface processes. The collection of atmospheric
+ physics parameterizations were originally used together as part of the GEOS-3
+ (Goddard Earth Observing System-3) GCM developed at the NASA/Goddard Global Modelling
+ and Assimilation Office (GMAO).
  % *************************************************************************
  % *************************************************************************
-Line 21 
 Moist Convective Processes:
+Line 24 
 Moist Convective Processes:
  \label{sec:fizhi:mc}
  Sub-grid scale cumulus convection is parameterized using the Relaxed Arakawa
- Schubert (RAS) scheme of Moorthi and Suarez (1992), which is a linearized Arakawa Schubert
+ Schubert (RAS) scheme of \cite{moorsz:92}, which is a linearized Arakawa Schubert
  type scheme.  RAS predicts the mass flux from an ensemble of clouds.  Each subensemble is identified
  by its entrainment rate and level of neutral bouyancy which are determined by the grid-scale properties.
-Line 43 
 where we have used the hydrostatic equat
+Line 46 
 where we have used the hydrostatic equat
  The entrainment parameter, $\lambda$, characterizes a particular subensemble based on its
  detrainment level, and is obtained by assuming that the level of detrainment is the level of neutral
  buoyancy, ie., the level at which the moist static energy of the cloud, $h_c$, is equal
- to the saturation moist static energy of the environment, $h^*$.  Following Moorthi and Suarez (1992),
+ to the saturation moist static energy of the environment, $h^*$.  Following \cite{moorsz:92},
  $\lambda$ may be written as
  \[
  \lambda = { {h_B - h^*_D} \over { {c_p \over g} {\int_{P_D}^{P_B}\theta(h^*_D-h)dP^{\kappa}}} } ,
-Line 101 
 $\alpha$ of the total adjustment. The pa
+Line 104 
 $\alpha$ of the total adjustment. The pa
  towards equillibrium.
  In addition to the RAS cumulus convection scheme, the fizhi package employs a
- Kessler-type scheme for the re-evaporation of falling rain (Sud and Molod, 1988), which
+ Kessler-type scheme for the re-evaporation of falling rain (\cite{sudm:88}), which
  correspondingly adjusts the temperature assuming $h$ is conserved. RAS in its current
  formulation assumes that all cloud water is deposited into the detrainment level as rain.
  All of the rain is available for re-evaporation, which begins in the level below detrainment.
-Line 166 
 RH_{min} & = & 0.75 \nonumber \\
+Line 169 
 RH_{min} & = & 0.75 \nonumber \\
  These cloud fractions are suppressed, however, in regions where the convective
  sub-cloud layer is conditionally unstable.  The functional form of $RH_c$ is shown in
- Figure (\ref{fig:fizhi:rhcrit}).
+ Figure (\ref{fig.rhcrit}).
  \begin{figure*}[htbp]
    \vspace{0.4in}
    \centerline{  \epsfysize=4.0in  \epsfbox{part6/rhcrit.ps}}
    \vspace{0.4in}
    \caption  [Critical Relative Humidity for Clouds.]
              {Critical Relative Humidity for Clouds.}
-   \label{fig:fizhi:rhcrit}
+   \label{fig.rhcrit}
  \end{figure*}
  The total cloud fraction in a grid box is determined by the larger of the two cloud fractions:
-Line 221 
 The solar constant value used in the pac
+Line 224 
 The solar constant value used in the pac
  and a $CO_2$ mixing ratio of 330 ppm.
  For the ozone mixing ratio, monthly mean zonally averaged
  climatological values specified as a function
- of latitude and height (Rosenfield, et al., 1987) are linearly interpolated to the current time.
+ of latitude and height (\cite{rosen:87}) are linearly interpolated to the current time.
  \paragraph{Shortwave Radiation}
-Line 231 
 heating due to the absoption by water va
+Line 234 
 heating due to the absoption by water va
  clouds, and aerosols and due to the
  scattering by clouds, aerosols, and gases.
  The shortwave radiative processes are described by
- Chou (1990,1992). This shortwave package
+ \cite{chou:90,chou:92}. This shortwave package
  uses the Delta-Eddington approximation to compute the
  bulk scattering properties of a single layer following King and Harshvardhan (JAS, 1986).
  The transmittance and reflectance of diffuse radiation
- follow the procedures of Sagan and Pollock (JGR, 1967) and Lacis and Hansen (JAS, 1974).
+ follow the procedures of Sagan and Pollock (JGR, 1967) and \cite{lhans:74}.
  Highly accurate heating rate calculations are obtained through the use
  of an optimal grouping strategy of spectral bands.  By grouping the UV and visible regions
-Line 305 
 cloud cover of all the layers in the gro
+Line 308 
 cloud cover of all the layers in the gro
  of a given layer is then scaled for both the direct (as a function of the
  solar zenith angle) and diffuse beam radiation
  so that the grouped layer reflectance is the same as the original reflectance.
- The solar flux is computed for each of the eight cloud realizations possible
+ The solar flux is computed for each of eight cloud realizations possible within this
- (see Figure \ref{fig:fizhi:cloud}) within this
  low/middle/high classification, and appropriately averaged to produce the net solar flux.
- \begin{figure*}[htbp]
-   \vspace{0.4in}
-   \centerline{  \epsfysize=4.0in  %\epsfbox{part6/rhcrit.ps}
-              }
-   \vspace{0.4in}
-   \caption  {Low-Middle-High Cloud Configurations}
-   \label{fig:fizhi:cloud}
- \end{figure*}
  \paragraph{Longwave Radiation}
- The longwave radiation package used in the fizhi package is thoroughly described by Chou and Suarez (1994).
+ The longwave radiation package used in the fizhi package is thoroughly described by \cite{chsz:94}.
  As described in that document, IR fluxes are computed due to absorption by water vapor, carbon
  dioxide, and ozone.  The spectral bands together with their absorbers and parameterization methods,
  configured for the fizhi package, are shown in Table \ref{tab:fizhi:longwave}.
-Line 357 
 Band & Spectral Range (cm$^{-1}$) & Abso
+Line 349 
 Band & Spectral Range (cm$^{-1}$) & Abso
  \end{tabular}
  \end{center}
  \vspace{0.1in}
- \caption{IR Spectral Bands, Absorbers, and Parameterization Method (from Chou and Suarez, 1994)}
+ \caption{IR Spectral Bands, Absorbers, and Parameterization Method (from \cite{chsz:94})}
  \label{tab:fizhi:longwave}
  \end{table}
-Line 428 
 The cloud fraction values are time-avera
+Line 420 
 The cloud fraction values are time-avera
  hours).  Therefore, in a time-averaged sense, both convective and large-scale
  cloudiness can exist in a given grid-box.
- Turbulence:
+ \paragraph{Turbulence}:
  Turbulence is parameterized in the fizhi package to account for its contribution to the
  vertical exchange of heat, moisture, and momentum.
-Line 459 
 Within the atmosphere, the time evolutio
+Line 451 
 Within the atmosphere, the time evolutio
  of second turbulent moments is explicitly modeled by representing the third moments in terms of
  the first and second moments.  This approach is known as a second-order closure modeling.
  To simplify and streamline the computation of the second moments, the level 2.5 assumption
- of Mellor and Yamada (1974) and Yamada (1977) is employed, in which only the turbulent
+ of Mellor and Yamada (1974) and \cite{yam:77} is employed, in which only the turbulent
  kinetic energy (TKE),
  \[ {\h}{q^2}={\overline{{u^{\prime}}^2}}+{\overline{{v^{\prime}}^2}}+{\overline{{w^{\prime}}^2}}, \]
-Line 493 
 of TKE.
+Line 485 
 of TKE.
  In the level 2.5 approach, the vertical fluxes of the scalars $\theta_v$ and $q$ and the
  wind components $u$ and $v$ are expressed in terms of the diffusion coefficients $K_h$ and
- $K_m$, respectively.  In the statisically realizable level 2.5 turbulence scheme of Helfand
+ $K_m$, respectively.  In the statisically realizable level 2.5 turbulence scheme of
- and Labraga (1988), these diffusion coefficients are expressed as
+ \cite{helflab:88}, these diffusion coefficients are expressed as
  \[
  K_h
-Line 569 
 where $\psi_h$ is the surface layer non-
+Line 561 
 where $\psi_h$ is the surface layer non-
  \]
  Here $\phi_h$ is the similarity function of $\zeta$, which expresses the stability dependance of
  the temperature and moisture gradients, and is specified differently for stable and unstable
- layers according to Helfand and Schubert, 1995.
+ layers according to \cite{helfschu:95}.
  $\psi_g$ is the non-dimensional temperature or moisture gradient in the viscous sublayer,
  which is the mosstly laminar region between the surface and the tops of the roughness
  elements, in which temperature and moisture gradients can be quite large.
- Based on Yaglom and Kader (1974):
+ Based on \cite{yagkad:74}:
  \[
  \psi_{g} = { 0.55 (Pr^{2/3} - 0.2) \over \nu^{1/2} }
  (h_{0}u_{*} - h_{0_{ref}}u_{*_{ref}})^{1/2}
-Line 588 
 The surface roughness length over oceans
+Line 580 
 The surface roughness length over oceans
  {z_0} = c_1u^3_* + c_2u^2_* + c_3u_* + c_4 + {c_5 \over {u_*}}
  \]
  where the constants are chosen to interpolate between the reciprocal relation of
- Kondo(1975) for weak winds, and the piecewise linear relation of Large and Pond(1981)
+ \cite{kondo:75} for weak winds, and the piecewise linear relation of \cite{larpond:81}
  for moderate to large winds.  Roughness lengths over land are specified
- from the climatology of Dorman and Sellers (1989).
+ from the climatology of \cite{dorsell:89}.
  For an unstable surface layer, the stability functions, chosen to interpolate between the
  condition of small values of $\beta$ and the convective limit, are the KEYPS function
- (Panofsky, 1973) for momentum, and its generalization for heat and moisture:
+ (\cite{pano:73}) for momentum, and its generalization for heat and moisture:
  \[
  {\phi_m}^4 - 18 \zeta {\phi_m}^3 = 1 \hspace{1cm} ; \hspace{1cm}
  {\phi_h}^2 - 18 \zeta {\phi_h}^3 = 1 \hspace{1cm} .
-Line 603 
 The function for heat and moisture assur
+Line 595 
 The function for heat and moisture assur
  speed approaches zero.
  For a stable surface layer, the stability functions are the observationally
- based functions of Clarke (1970),  slightly modified for
+ based functions of \cite{clarke:70},  slightly modified for
  the momemtum flux:
  \[
  {\phi_m} = { { 1 + 5 {{\zeta}_1} } \over { 1 + 0.00794 {{\zeta}_1}
-Line 661 
 be $3 \hspace{.1cm} m$ where sea ice is
+Line 653 
 be $3 \hspace{.1cm} m$ where sea ice is
  surface temperature of the ice.
  $C_g$ is the total heat capacity of the ground, obtained by solving a heat diffusion equation
- for the penetration of the diurnal cycle into the ground (Blackadar, 1977), and is given by:
+ for the penetration of the diurnal cycle into the ground (\cite{black:77}), and is given by:
  \[
  C_g = \sqrt{ {\lambda C_s \over 2\omega} } = \sqrt{(0.386 + 0.536W + 0.15W^2)2\times10^{-3}
  {86400 \over 2 \pi} } \, \, .
-Line 676 
 is a function of the ground wetness, $W$
+Line 668 
 is a function of the ground wetness, $W$
  Land Surface Processes:
  \paragraph{Surface Type}
- The fizhi package surface Types are designated using the Koster-Suarez (1992) mosaic
+ The fizhi package surface Types are designated using the Koster-Suarez (\cite{ks:91,ks:92})
- philosophy which allows multiple ``tiles'', or multiple surface types, in any one
+ Land Surface Model (LSM) mosaic philosophy which allows multiple ``tiles'', or multiple surface
- grid cell. The Koster-Suarez Land Surface Model (LSM) surface type classifications
+ types, in any one grid cell. The Koster-Suarez LSM surface type classifications
  are shown in Table \ref{tab:fizhi:surftype}. The surface types and the percent of the grid
  cell occupied by any surface type were derived from the surface classification of
- Defries and Townshend (1994), and information about the location of permanent
+ \cite{deftow:94}, and information about the location of permanent
- ice was obtained from the classifications of Dorman and Sellers (1989).
+ ice was obtained from the classifications of \cite{dorsell:89}.
- The surface type for the \txt GCM grid is shown in Figure \ref{fig:fizhi:surftype}.
+ The surface type map for a $1^\circ$ grid is shown in Figure \ref{fig:fizhi:surftype}.
  The determination of the land or sea category of surface type was made from NCAR's
 minute by 10 minute Navy topography
  dataset, which includes information about the percentage of water-cover at any point.
- The data were averaged to the model's \fxf and \txt grid resolutions,
+ The data were averaged to the model's grid resolutions,
  and any grid-box whose averaged water percentage was $\geq 60 \%$ was
- defined as a water point. The \fxf grid Land-Water designation was further modified
+ defined as a water point. The Land-Water designation was further modified
  subjectively to ensure sufficient representation from small but isolated land and water regions.
  \begin{table}
-Line 720 
 and surface albedo.}
+Line 712 
 and surface albedo.}
  \begin{figure*}[htbp]
-   \centerline{  \epsfysize=7in  \epsfbox{part6/surftypes.ps}}
+   \begin{center}
-   \vspace{0.3in}
+   \rotatebox{270}{\resizebox{90mm}{!}{\includegraphics{part6/surftypes.eps}}}
-   \caption  {Surface Type Compinations at \txt resolution.}
+   \rotatebox{270}{\resizebox{100mm}{!}{\includegraphics{part6/surftypes.descrip.eps}}}
+   \end{center}
+   \vspace{0.2in}
+   \caption  {Surface Type Combinations at $1^\circ$ resolution.}
    \label{fig:fizhi:surftype}
  \end{figure*}
- \begin{figure*}[htbp]
+ % \rotatebox{270}{\centerline{  \epsfysize=4in  \epsfbox{part6/surftypes.eps}}}
-   \centerline{  \epsfysize=7in  \epsfbox{part6/surftypes.descrip.ps}}
+ % \rotatebox{270}{\centerline{  \epsfysize=4in  \epsfbox{part6/surftypes.descrip.eps}}}
-   \vspace{0.3in}
+ %\begin{figure*}[htbp]
-   \caption  {Surface Type Descriptions.}
+ %  \centerline{  \epsfysize=4in  \epsfbox{part6/surftypes.descrip.ps}}
-   \label{fig:fizhi:surftype.desc}
+ %  \vspace{0.3in}
- \end{figure*}
+ %  \caption  {Surface Type Descriptions.}
+ %  \label{fig:fizhi:surftype.desc}
+ %\end{figure*}
  \paragraph{Surface Roughness}
  The surface roughness length over oceans is computed iteratively with the wind
- stress by the surface layer parameterization (Helfand and Schubert, 1991).
+ stress by the surface layer parameterization (\cite{helfschu:95}).
- It employs an interpolation between the functions of Large and Pond (1981)
+ It employs an interpolation between the functions of \cite{larpond:81}
- for high winds and of Kondo (1975) for weak winds.
+ for high winds and of \cite{kondo:75} for weak winds.
  \paragraph{Albedo}
- The surface albedo computation, described in Koster and Suarez (1991),
+ The surface albedo computation, described in \cite{ks:91},
  employs the ``two stream'' approximation used in Sellers' (1987) Simple Biosphere (SiB)
  Model which distinguishes between the direct and diffuse albedos in the visible
  and in the near infra-red spectral ranges. The albedos are functions of the observed
-Line 751 
 sun), the greenness fraction, the vegeta
+Line 748 
 sun), the greenness fraction, the vegeta
  Modifications are made to account for the presence of snow, and its depth relative
  to the height of the vegetation elements.
- Gravity Wave Drag:
+ \paragraph{Gravity Wave Drag}
- The fizhi package employs the gravity wave drag scheme of Zhou et al. (1996).
+ The fizhi package employs the gravity wave drag scheme of \cite{zhouetal:95}).
  This scheme is a modified version of Vernekar et al. (1992),
  which was based on Alpert et al. (1988) and Helfand et al. (1987).
  In this version, the gravity wave stress at the surface is
-Line 770 
 A modification introduced by Zhou et al.
+Line 767 
 A modification introduced by Zhou et al.
  escape through the top of the model, although this effect is small for the current 70-level model.
  The subgrid scale standard deviation is defined by $h$, and is not allowed to exceed 400 m.
- The effects of using this scheme within a GCM are shown in Takacs and Suarez (1996).
+ The effects of using this scheme within a GCM are shown in \cite{taksz:96}.
  Experiments using the gravity wave drag parameterization yielded significant and
  beneficial impacts on both the time-mean flow and the transient statistics of the
  a GCM climatology, and have eliminated most of the worst dynamically driven biases
-Line 794 
 fields include:  sea surface temperature
+Line 791 
 fields include:  sea surface temperature
  vegetation index, and the radiation-related background levels of: ozone, carbon dioxide,
  and stratospheric moisture.
- Boundary condition data sets are available at the model's \fxf and \txt
+ Boundary condition data sets are available at the model's
  resolutions for either climatological or yearly varying conditions.
  Any frequency of boundary condition data can be used in the fizhi package;
  however, the current selection of data is summarized in Table \ref{tab:fizhi:bcdata}\@.
  The time mean values are interpolated during each model timestep to the
- current time. Future model versions will incorporate boundary conditions at
+ current time.
- higher spatial \mbox{($1^\circ$ x $1^\circ$)} resolutions.
  \begin{table}[htb]
  \begin{center}
-Line 827 
 current years and frequencies available.
+Line 823 
 current years and frequencies available.
  Surface geopotential heights are provided from an averaging of the Navy 10 minute
  by 10 minute dataset supplied by the National Center for Atmospheric Research (NCAR) to the
  model's grid resolution. The original topography is first rotated to the proper grid-orientation
- which is being run, and then
+ which is being run, and then  averages the data to the model resolution.
- averages the data to the model resolution.
- The averaged topography is then passed through a Lanczos (1966) filter in both dimensions
- which removes the smallest
- scales while inhibiting Gibbs phenomena.
- In one dimension, we may define a cyclic function in $x$ as:
- \begin{equation}
- f(x) = {a_0 \over 2} + \sum_{k=1}^N \left( a_k \cos(kx) + b_k \sin(kx) \right)
- \label{eq:fizhi:filt}
- \end{equation}
- where $N = { {\rm IM} \over 2 }$ and ${\rm IM}$ is the total number of points in the $x$ direction.
- Defining $\Delta x = { 2 \pi \over {\rm IM}}$, we may define the average of $f(x)$ over a
- $2 \Delta x$ region as:
- \begin{equation}
- \overline {f(x)} = {1 \over {2 \Delta x}} \int_{x-\Delta x}^{x+\Delta x} f(x^{\prime}) dx^{\prime}
- \label{eq:fizhi:fave1}
- \end{equation}
- Using equation (\ref{eq:fizhi:filt}) in equation (\ref{eq:fizhi:fave1}) and integrating, we may write:
- \begin{equation}
- \overline {f(x)} = {a_0 \over 2} + {1 \over {2 \Delta x}}
- \sum_{k=1}^N \left [
- \left. a_k { \sin(kx^{\prime}) \over k } \right /_{x-\Delta x}^{x+\Delta x} -
- \left. b_k { \cos(kx^{\prime}) \over k } \right /_{x-\Delta x}^{x+\Delta x}
- \right]
- \end{equation}
- or
- \begin{equation}
- \overline {f(x)} = {a_0 \over 2} + \sum_{k=1}^N {\sin(k \Delta x) \over {k \Delta x}}
- \left( a_k \cos(kx) + b_k \sin(kx) \right)
- \label{eq:fizhi:fave2}
- \end{equation}
- Thus, the Fourier wave amplitudes are simply modified by the Lanczos filter response
- function ${\sin(k\Delta x) \over {k \Delta x}}$.  This may be compared with an $mth$-order
- Shapiro (1970) filter response function, defined as $1-\sin^m({k \Delta x \over 2})$,
- shown in Figure \ref{fig:fizhi:lanczos}.
- It should be noted that negative values in the topography resulting from
- the filtering procedure are {\em not} filled.
- \begin{figure*}[htbp]
-   \centerline{  \epsfysize=7.0in  \epsfbox{part6/lanczos.ps}}
-   \caption{ \label{fig:fizhi:lanczos} Comparison between the Lanczos and $mth$-order Shapiro filter
-   response functions for $m$ = 2, 4, and 8. }
- \end{figure*}
- The standard deviation of the subgrid-scale topography
+ The standard deviation of the subgrid-scale topography is computed by interpolating the 10 minute
- is computed from a modified version of the the Navy 10 minute by 10 minute dataset.
+ data to the model's resolution and re-interpolating back to the 10 minute by 10 minute resolution.
- The 10 minute by 10 minute topography is passed through a wavelet
- filter in both dimensions which removes the scale smaller than 20 minutes.
- The topography is then averaged to $1^\circ x 1^\circ$ grid resolution, and then
- re-interpolated back to the 10 minute by 10 minute resolution.
  The sub-grid scale variance is constructed based on this smoothed dataset.
  \paragraph{Upper Level Moisture}
  The fizhi package uses climatological water vapor data above 100 mb from the Stratospheric Aerosol and Gas
  Experiment (SAGE) as input into the model's radiation packages.  The SAGE data is archived
- as monthly zonal means at 5$^\circ$ latitudinal resolution.  The data is interpolated to the
+ as monthly zonal means at $5^\circ$ latitudinal resolution.  The data is interpolated to the
  model's grid location and current time, and blended with the GCM's moisture data.  Below 300 mb,
  the model's moisture data is used.  Above 100 mb, the SAGE data is used.  Between 100 and 300 mb,
  a linear interpolation (in pressure) is performed using the data from SAGE and the GCM.
-Line 898 
 a linear interpolation (in pressure) is
+Line 842 
 a linear interpolation (in pressure) is
  \subsubsection{Fizhi Diagnostics}
  Fizhi Diagnostic Menu:
- \label{sec:fizhi-diagnostics:menu}
+ \label{sec:pkg:fizhi:diagnostics}
  \begin{tabular}{llll}
  \hline\hline
-Line 1430 
 Fizhi Diagnostic Description:
+Line 1374 
 Fizhi Diagnostic Description:
  In this section we list and describe the diagnostic quantities available within the
  GCM.  The diagnostics are listed in the order that they appear in the
- Diagnostic Menu, Section \ref{sec:fizhi-diagnostics:menu}.
+ Diagnostic Menu, Section \ref{sec:pkg:fizhi:diagnostics}.
  In all cases, each diagnostic as currently archived on the output datasets
  is time-averaged over its diagnostic output frequency:
-Line 1588 
 $h_{0} = 30z_{0}$ with a maximum value o
+Line 1532 
 $h_{0} = 30z_{0}$ with a maximum value o
  \noindent
  $\phi_h$ is the similarity function of $\zeta$, which expresses the stability dependance of
  the temperature and moisture gradients, specified differently for stable and unstable
- layers according to Helfand and Schubert, 1993. k is the Von Karman constant, $\zeta$ is the
+ layers according to \cite{helfschu:95}. k is the Von Karman constant, $\zeta$ is the
  non-dimensional stability parameter, Pr is the Prandtl number for air, $\nu$ is the molecular
  viscosity, $z_{0}$ is the surface roughness length, $u_*$ is the surface stress velocity
  (see diagnostic number 67), and the subscript ref refers to a reference value.
-Line 1610 
 where $\psi_m$ is the surface layer non-
+Line 1554 
 where $\psi_m$ is the surface layer non-
  \noindent
  $\phi_m$ is the similarity function of $\zeta$, which expresses the stability dependance of
  the temperature and moisture gradients, specified differently for stable and unstable layers
- according to Helfand and Schubert, 1993. k is the Von Karman constant, $\zeta$ is the
+ according to \cite{helfschu:95}. k is the Von Karman constant, $\zeta$ is the
  non-dimensional stability parameter, $u_*$ is the surface stress velocity
  (see diagnostic number 67), and $W_s$ is the magnitude of the surface layer wind.
  \\
-Line 1622 
 non-dimensional stability parameter, $u_
+Line 1566 
 non-dimensional stability parameter, $u_
  In the level 2.5 version of the Mellor-Yamada (1974) hierarchy, the turbulent heat or
  moisture flux for the atmosphere above the surface layer can be expressed as a turbulent
  diffusion coefficient $K_h$ times the negative of the gradient of potential temperature
- or moisture. In the Helfand and Labraga (1988) adaptation of this closure, $K_h$
+ or moisture. In the \cite{helflab:88} adaptation of this closure, $K_h$
  takes the form:
  \[
  {\bf ET} = K_h = -{( {\overline{w^{\prime}\theta_v^{\prime}}}) \over {\pp{\theta_v}{z}} }
-Line 1641 
 are functions of the Richardson number.
+Line 1585 
 are functions of the Richardson number.
  \noindent
  For the detailed equations and derivations of the modified level 2.5 closure scheme,
- see Helfand and Labraga, 1988.
+ see \cite{helflab:88}.
  \noindent
  In the surface layer, ${\bf {ET}}$ is the exchange coefficient for heat and moisture,
-Line 1663 
 and $W_s$ is the magnitude of the surfac
+Line 1607 
 and $W_s$ is the magnitude of the surfac
  In the level 2.5 version of the Mellor-Yamada (1974) hierarchy, the turbulent heat
  momentum flux for the atmosphere above the surface layer can be expressed as a turbulent
  diffusion coefficient $K_m$ times the negative of the gradient of the u-wind.
- In the Helfand and Labraga (1988) adaptation of this closure, $K_m$
+ In the \cite{helflab:88} adaptation of this closure, $K_m$
  takes the form:
  \[
  {\bf EU} = K_m = -{( {\overline{u^{\prime}w^{\prime}}}) \over {\pp{U}{z}} }
-Line 1683 
 are functions of the Richardson number.
+Line 1627 
 are functions of the Richardson number.
  \noindent
  For the detailed equations and derivations of the modified level 2.5 closure scheme,
- see Helfand and Labraga, 1988.
+ see \cite{helflab:88}.
  \noindent
  In the surface layer, ${\bf {EU}}$ is the exchange coefficient for momentum,
-Line 2073 
 net surface upward longwave radiative fl
+Line 2017 
 net surface upward longwave radiative fl
  sea ice, $H$ is the upward sensible heat flux, $LE$ is the upward latent heat
  flux, and $C_g$ is the total heat capacity of the ground.
  $C_g$ is obtained by solving a heat diffusion equation
- for the penetration of the diurnal cycle into the ground (Blackadar, 1977), and is given by:
+ for the penetration of the diurnal cycle into the ground (\cite{black:77}), and is given by:
  \[
  C_g = \sqrt{ {\lambda C_s \over {2 \omega} } } = \sqrt{(0.386 + 0.536W + 0.15W^2)2x10^{-3}
  { 86400. \over {2 \pi} } } \, \, .
-Line 2428 
 number 10), and $W_s$ is the surface win
+Line 2372 
 number 10), and $W_s$ is the surface win
  \noindent
  Over the land surface, the surface roughness length is interpolated to the local
- time from the monthly mean data of Dorman and Sellers (1989). Over the ocean,
+ time from the monthly mean data of \cite{dorsell:89}. Over the ocean,
  the roughness length is a function of the surface-stress velocity, $u_*$.
  \[
  {\bf Z0} = c_1u^3_* + c_2u^2_* + c_3u_* + c_4 + {c_5 \over {u_*}}
-Line 2436 
 the roughness length is a function of th
+Line 2380 
 the roughness length is a function of th
  \noindent
  where the constants are chosen to interpolate between the reciprocal relation of
- Kondo(1975) for weak winds, and the piecewise linear relation of Large and Pond(1981)
+ \cite{kondo:75} for weak winds, and the piecewise linear relation of \cite{larpond:81}
  for moderate to large winds.
  \\

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