Merge pull request #54 from olivierbonte/fix/correcting_docs

Fix minor mistakes in documentation, Thanks @olivierbonte

Author: bgctw

docs/src/index.md

@@ -33,12 +33,16 @@ Pages = ["boundary_layer_conductance.md",]
 Pages = ["aerodynamic_conductance.md",]
 ```
 
+## Surface Conductance
+```@index
+Pages = ["surface_conductance.md",]
+```
+
 ## Evapotranspiration
 ```@index
 Pages = ["evapotranspiration.md",]
 ```
 
-
 ## Global radiation
 ```@index
 Pages = ["global_radiation.md",]

src/boundary_layer_conductance.jl

@@ -208,7 +208,11 @@ Boundary Layer Conductance using constant kB^(-1) value for heat transfer.
 - `constants=`[`BigleafConstants`](@ref)`()`
  
 # Details
-Rb_h computed by ``kB_h/(k * ustar)``, where k is the von Karman constant.
+Rb_h computed by :
+
+``kB_h/(k * ustar)``
+
+where k is the von Karman constant.
 """
 function Gb_constant_kB1(ustar, kB_h; constants=BigleafConstants())
   ismissing(ustar) && return(missing)
@@ -325,7 +329,7 @@ and ``R_{eh}`` is the Reynolds number for leaves:
 
 ``R_{eh} = D_l \\, wind(z_h) / v``
  
-k_{Bs-1}, the k_{B-1} value for bare soil surface, is calculated according 
+``k_{Bs-1}``, the ``k_{B-1}`` value for bare soil surface, is calculated according 
 to Su et al. 2001:
 
 ``k_{Bs-1} = 2.46(Re)^{0.25} - ln(7.4)``

src/evapotranspiration.jl

@@ -262,15 +262,15 @@ where ``\\Omega`` is the decoupling coefficient as calculated from
 the ET rate that would occur under uncoupled conditions, where the budget
 is dominated by radiation (when Ga -> 0):
 
-``ET_{eq} = (\\Delta \\, (R_n - G - S) \\, \\lambda) / ( \\Delta \\gamma)``
+``ET_{eq} = (\\Delta \\, (R_n - G - S)) / (\\lambda \\, (\\Delta + \\gamma))``
 
 where ``\\Delta`` is the slope of the saturation vapor pressur(kPa K-1),
 ``\\lambda`` is the latent heat of vaporization (J kg-1), and ``\\gamma``
 is the psychrometric constant (kPa K-1).
 `ET_imp` is the imposed evapotranspiration rate, the ET rate
 that would occur under fully coupled conditions (when Ga -> inf):
 
-``ET_{imp} = (\\rho \\, c_p \\, \\mathit{VPD} ~ G_s \\, \\lambda) / \\gamma``
+``ET_{imp} = (\\rho \\, c_p \\, \\mathit{VPD} ~ G_s) / (\\lambda \\, \\gamma)``
 
 where ``\\rho`` is the air density (kg m-3).
  

src/surface_conductance.jl

@@ -33,11 +33,11 @@ additional for InversePenmanMonteith
 For `InversePenmanMonteith()`, surface conductance (Gs) in m s-1 
 is calculated from the inverted Penman-Monteith equation:
 
-``G_s = ( LE \\. G_a \\, \\gamma ) / ( \\Delta \\, A + \\rho \\, c_p \\, G_a \\, VPD - 
+``G_s = ( LE \\, G_a \\, \\gamma ) / ( \\Delta \\, A + \\rho \\, c_p \\, G_a \\, VPD - 
 LE \\, (\\Delta + \\gamma ))``
 
 Where ``\\gamma`` is the psychrometric constant (kPa K-1), ``\\Delta`` is the slope of the 
-saturation vapor pressure curve (kPa K^-1), and ``\\rho`` is air density (kg m-3).
+saturation vapor pressure curve (kPa K-1), and ``\\rho`` is air density (kg m-3).
 Available energy (A) is defined as ``A = R_n - G - S``. 
 
 Ground heat flux and total storage flux can be provided as scalars or vectors of