Clean out another duplicate ref.

docs/ocean.bib

@@ -10,18 +10,6 @@ @article{Adcroft2004
 	journal = {Ocean Modelling}
 }
 
-@article{Adcroft2019,
-	doi = {10.1029/2019ms001726},
-	year = 2019,
-	publisher = {American Geophysical Union ({AGU})},
-	volume = {11},
-	number = {10},
-	pages = {3167--3211},
-	author = {A. Adcroft and W. Anderson and V. Balaji and C. Blanton and M. Bushuk and C. O. Dufour and J. P. Dunne and S. M. Griffies and R. Hallberg and M. J. Harrison and I. M. Held and M. F. Jansen and J. G. John and J. P. Krasting and A. R. Langenhorst and S. Legg and Z. Liang and C. McHugh and A. Radhakrishnan and B. G. Reichl and T. Rosati and B. L. Samuels and A. Shao and R. Stouffer and M. Winton and A. T. Wittenberg and B. Xiang and N. Zadeh and R. Zhang},
-	title = {The {GFDL} Global Ocean and Sea Ice Model {OM}4.0: Model Description and Simulation Features},
-	journal = {J. Adv. Mod. Earth Sys.}
-}
-
 @article{Campin2004,
 	doi = {10.1016/s1463-5003(03)00009-x},
 	year = 2004,

docs/zotero.bib

@@ -967,7 +967,7 @@ @article{bitz1999
 	pages = {15669--15677}
 }
 
-@inproceedings{briegleb2007,
+@incollection{briegleb2007,
 	series = {Technical {Note}},
 	title = {A {Delta}-{Eddington} {Mutiple} {Scattering} {Parameterization} for {Solar} {Radiation} in the {Sea} {Ice} {Component} of the {Community} {Climate} {System} {Model} {\textbar} {OpenSky} {Repository}},
 	url = {http://opensky.ucar.edu/islandora/object/technotes:484},
@@ -2447,7 +2447,7 @@ @article{russell1981
 	doi = {10.1175/1520-0450(1981)020<1483:ANFDSF>2.0.CO;2}
 }
 
-@inproceedings{huynh1997,
+@incollection{huynh1997,
 	title = {Schemes and constraints for advection},
 	booktitle = {Fifteenth International Conference on Numerical
 	  Methods in Fluid Dynamics},
@@ -2564,7 +2564,7 @@ @article{marshall2010
 	doi = {10.1016/j.ocemod.2010.02.001}
 }
 
-@inproceedings{millero1978,
+@incollection{millero1978,
 	author = {Millero, F.J.},
 	title = {Freezing point of seawater},
 	note = {Annex 6},
@@ -2820,7 +2820,7 @@ @article{Large2001
 	pages={518–536}
 }
 
-@inproceedings{Smagorinsky1993,
+@incollection{Smagorinsky1993,
 	author={Joseph Smagorinsky},
 	year={1993},
 	title={Some historical remarks on the use of non-linear viscosities},
@@ -2884,7 +2884,7 @@ @article{Wang2012-2
 	pages={190--199}
 }
 
-@inproceedings{Hallberg2003,
+@incollection{Hallberg2003,
 	title={The ability of large-scale ocean models to accept parameterizations of boundary mixing, and a description of a refined bulk mixed-layer model},
 	author={Robert Hallberg},
 	year={2003},

src/parameterizations/lateral/MOM_hor_visc.F90

@@ -2044,9 +2044,9 @@ subroutine horizontal_viscosity(u, v, h, uh, vh, diffu, diffv, MEKE, VarMix, G,
 
 end subroutine horizontal_viscosity
 
-!> Allocates space for and calculates static variables used by horizontal_viscosity().
+!> Allocates space for and calculates static variables used by horizontal_viscosity.
 !! hor_visc_init calculates and stores the values of a number of metric functions that
-!! are used in horizontal_viscosity().
+!! are used in horizontal_viscosity.
 subroutine hor_visc_init(Time, G, GV, US, param_file, diag, CS, ADp)
   type(time_type),         intent(in)    :: Time !< Current model time.
   type(ocean_grid_type),   intent(inout) :: G    !< The ocean's grid structure.
@@ -3259,7 +3259,7 @@ end subroutine hor_visc_end
 !! \f}
 !!
 !! The viscosity \f$\kappa_h\f$ may either be a constant or variable. For example,
-!! \f$\kappa_h\f$ may vary with the shear, as proposed by Smagorinsky (1993).
+!! \f$\kappa_h\f$ may vary with the shear, as proposed by \cite Smagorinsky1993.
 !!
 !! The accelerations resulting form the divergence of the stress tensor are
 !! \f{eqnarray*}{
@@ -3357,8 +3357,8 @@ end subroutine hor_visc_end
 !!
 !! \subsection section_anisotropic_viscosity Anisotropic viscosity
 !!
-!! \cite Large2001, proposed enhancing viscosity in a particular direction and the
-!! approach was generalized in Smith and McWilliams, 2003. We use the second form of their
+!! \cite Large2001 proposed enhancing viscosity in a particular direction and the
+!! approach was generalized in \cite Smith2003. We use the second form of their
 !! two coefficient anisotropic viscosity (section 4.3). We also replace their
 !! \f$A^\prime\f$ and $D$ such that \f$2A^\prime = 2 \kappa_h + D\f$ and
 !! \f$\kappa_a = D\f$ so that \f$\kappa_h\f$ can be considered the isotropic

src/parameterizations/lateral/MOM_interface_filter.F90

@@ -480,7 +480,7 @@ end subroutine interface_filter_end
 !! filter, depending on the order of the filter, or to the slope for a Laplacian
 !! filter
 !! \f[
-!! \vec{\psi} = - \kappa_h {\nabla \eta - \eta_smooth}
+!! \vec{\psi} = - \kappa_h {\nabla \eta - \eta_{smooth}}
 !! \f]
 !!
 !! The result of the above expression is subsequently bounded by minimum and maximum values, including a

src/parameterizations/lateral/MOM_lateral_mixing_coeffs.F90

@@ -1734,8 +1734,8 @@ end subroutine VarMix_end
 !! r(\Delta,L_d) = \frac{1}{1+(\alpha R)^p}
 !! \f]
 !!
-!! The resolution function can be applied independently to thickness diffusion (module mom_thickness_diffuse),
-!! tracer diffusion (mom_tracer_hordiff) lateral viscosity (mom_hor_visc).
+!! The resolution function can be applied independently to thickness diffusion \(module mom_thickness_diffuse\),
+!! tracer diffusion \(mom_tracer_hordiff\) lateral viscosity \(mom_hor_visc\).
 !!
 !! Robert Hallberg, 2013: Using a resolution function to regulate parameterizations of oceanic mesoscale eddy effects.
 !! Ocean Modelling, 71, pp 92-103.  http://dx.doi.org/10.1016/j.ocemod.2013.08.007
@@ -1757,7 +1757,7 @@ end subroutine VarMix_end
 !! \section section_Vicbeck Visbeck diffusivity
 !!
 !! This module also calculates factors used in setting the thickness diffusivity similar to a Visbeck et al., 1997,
-!! scheme.  The factors are combined in mom_thickness_diffuse::thickness_diffuse() but calculated in this module.
+!! scheme.  The factors are combined in mom_thickness_diffuse::thickness_diffuse but calculated in this module.
 !!
 !! \f[
 !! \kappa_h = \alpha_s L_s^2 S N

src/parameterizations/lateral/MOM_mixed_layer_restrat.F90

@@ -1971,15 +1971,15 @@ end function test_answer
 !! \cite Hallberg2003, which this new parameterization surpasses, which
 !! in turn is based on the sub-inertial mixed layer theory of \cite Young1994.
 !! There is no net horizontal volume transport due to this parameterization, and
-!! no direct effect below the mixed layer. A revised of the parameterization by
-!! \cite Bodner2023, is also available as an option.
+!! no direct effect below the mixed layer. A revised version of the parameterization by
+!! \cite Bodner2023 is also available as an option.
 !!
 !! This parameterization sets the restratification timescale to agree with
 !! high-resolution studies of mixed layer restratification.
 !!
-!! The run-time parameter FOX_KEMPER_ML_RESTRAT_COEF is a non-dimensional number of
+!! The run-time parameter <code>FOX_KEMPER_ML_RESTRAT_COEF</code> is a non-dimensional number of
 !! order a few tens, proportional to the ratio of the deformation radius or the
-!! grid scale (whichever is smaller to the dominant horizontal length-scale of the
+!! grid scale (whichever is smaller) to the dominant horizontal length-scale of the
 !! sub-meso-scale mixed layer instabilities.
 !!
 !! \subsection section_mle_nutshell "Sub-meso" in a nutshell
@@ -2011,14 +2011,15 @@ end function test_answer
 !! \f$ \tau \f$ is a time-scale for mixing momentum across the mixed layer.
 !! \f$ l_f \f$ is thought to be of order hundreds of meters.
 !!
-!! The upscaling factor \f$ \frac{\Delta s}{l_f} \f$ can be a global constant, model parameter FOX_KEMPER_ML_RESTRAT,
-!! so that in practice the parameterization is:
+!! The upscaling factor \f$ \frac{\Delta s}{l_f} \f$ can be a global constant, model parameter
+!! <code>FOX_KEMPER_ML_RESTRAT</code>, so that in practice the parameterization is:
 !! \f[
 !!    {\bf \Psi} = C_e \Gamma_\Delta \frac{ H^2 \nabla \bar{b} \times \hat{\bf z} }{ \sqrt{ f^2 + \tau^{-2}} } \mu(z)
 !! \f]
 !! with non-unity \f$ \Gamma_\Delta \f$.
 !!
 !! \f$ C_e \f$ is hard-coded as 0.0625. \f$ \tau \f$ is calculated from the surface friction velocity \f$ u^* \f$.
+!!
 !! \todo Explain expression for momentum mixing time-scale.
 !!
 !! | Symbol                       | Module parameter      |
@@ -2102,7 +2103,7 @@ end function test_answer
 !! | \f$ \tau_{h+} \f$            | MLE\%BLD_GROWING_TFILTER  |
 !! | \f$ \tau_{h-} \f$            | MLE\%BLD_DECAYING_TFILTER |
 !! | \f$ \tau_{H+} \f$            | MLE\%MLD_GROWING_TFILTER  |
-!! | \f$ \tau_{H-} \f$            | MLE\%BLD_DECAYING_TFILTER |
+!! | \f$ \tau_{H-} \f$            | MLE\%MLD_DECAYING_TFILTER |
 !!
 !! \subsection section_mle_ref References
 !!

src/parameterizations/lateral/MOM_self_attr_load.F90

@@ -251,12 +251,12 @@ end subroutine SAL_end
 !! (rather, it should be bottom pressure anomaly). SAL is primarily used for fast evolving processes like tides or
 !! storm surges, but the effect applies to all motions.
 !!
-!!     If SAL_SCALAR_APPROX is true, a scalar approximation is applied (\cite Accad1978) and the SAL is simply
+!! If SAL_SCALAR_APPROX is true, a scalar approximation is applied [\cite Accad1978] and the SAL is simply
 !! a fraction (set by SAL_SCALAR_VALUE, usually around 10% for global tides) of local SSH . For tides, the scalar
 !! approximation can also be used to iterate the SAL to convergence [see USE_PREVIOUS_TIDES in MOM_tidal_forcing,
 !! \cite Arbic2004].
 !!
-!!    If SAL_HARMONICS is true, a more accurate online spherical harmonic transforms are used to calculate SAL.
+!! If SAL_HARMONICS is true, a more accurate online spherical harmonic transforms are used to calculate SAL.
 !! Subroutines in module MOM_spherical_harmonics are called and the degree of spherical harmonic transforms is set by
 !! SAL_HARMONICS_DEGREE. The algorithm is based on SAL calculation in Model for Prediction Across Scales (MPAS)-Ocean
 !! developed by Los Alamos National Laboratory and University of Michigan [\cite Barton2022 and \cite Brus2023].