diff --git a/dev/model_docs/vertical/shared_processes.html b/dev/model_docs/vertical/shared_processes.html
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--- a/dev/model_docs/vertical/shared_processes.html
+++ b/dev/model_docs/vertical/shared_processes.html
@@ -398,7 +398,7 @@ <h1 class="title">Shared processes</h1>
 <h2 class="anchored" data-anchor-id="snow-and-glaciers">Snow and glaciers</h2>
 <section id="snow-modelling" class="level3">
 <h3 class="anchored" data-anchor-id="snow-modelling">Snow modelling</h3>
-<p>If the air temperature, <span class="math inline">\(T_a\)</span>, is below a user-defined threshold <code>tt</code> <span class="math inline">\(\SIb{}{\degree C}\)</span> precipitation occurs as snowfall, whereas it occurs as rainfall if <span class="math inline">\(T_a ≥ \mathrm{tt}\)</span>. A another parameter <code>tti</code> defines how precipitation can occur partly as rain or snowfall.</p>
+<p>If the air temperature, <span class="math inline">\(T_a\)</span>, is below a user-defined threshold <code>tt</code> <span class="math inline">\(\SIb{}{\degree C}\)</span> precipitation occurs as snowfall, whereas it occurs as rainfall if <span class="math inline">\(T_a ≥ \mathrm{tt}\)</span>. Another parameter <code>tti</code> defines how precipitation can occur partly as rain or snowfall.</p>
 <div class="quarto-figure quarto-figure-center">
 <figure class="figure">
 <p><img src="../../images/snowfall.png" class="img-fluid figure-img"></p>
diff --git a/dev/search.json b/dev/search.json
index eee716a8d..4c1708164 100644
--- a/dev/search.json
+++ b/dev/search.json
@@ -1341,7 +1341,7 @@
     "href": "model_docs/vertical/shared_processes.html",
     "title": "Shared processes",
     "section": "",
-    "text": "If the air temperature, \\(T_a\\), is below a user-defined threshold tt \\(\\SIb{}{\\degree C}\\) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥ \\mathrm{tt}\\). A another parameter tti defines how precipitation can occur partly as rain or snowfall.\n\n\n\nDivision between snow and precipitation based on the threshold temperature\n\n\n\nIf precipitation occurs as snowfall, it is added to the dry snow component within the snow pack. Otherwise it ends up in the free water reservoir, which represents the liquid water content of the snow pack. Between the two components of the snow pack, interactions take place, either through snow melt (if temperatures are above a threshold tt) or through snow refreezing (if temperatures are below threshold tt).\nThe respective rates of snow melt and refreezing are:\n\\[\n\\begin{align*}\n    Q_m &=& \\subtext{\\mathrm{cf}}{max}(T_a−\\mathrm{tt})\\, &&T_a &gt; \\mathrm{tt} \\\\\n    Q_r &=& \\subtext{\\mathrm{cf}}{max} \\, \\mathrm{cf}_r(\\mathrm{tt}−T_a) &&T_a &lt; \\mathrm{tt}\n\\end{align*}\n\\]\nwhere \\(Q_m\\) is the rate of snow melt, \\(Q_r\\) is the rate of snow refreezing, and \\(\\SIb{\\subtext{\\mathrm{cf}}{max}}{mm\\;(\\degree C)^{-1} day^{-1}}\\) and \\(\\mathrm{cf}_r\\) are user defined model parameters (the melting factor and the refreezing factor respectively).\nThe fraction of liquid water in the snow pack is at most equal to a user defined fraction, whc, of the water equivalent of the dry snow content. If the liquid water concentration exceeds whc, either through snow melt or incoming rainfall, the surplus water (rainfall) becomes available for infiltration into the soil:\nsnowwater = snowwater - refreezing  # free water content in snow\nmaxsnowwater = snow * whc  # max water in the snow\nsnowwater = snowwater + snowmelt + rainfall  # add all water and potentially supersaturate the snowpack\nrainfall = max(snowwater - maxsnowwater, 0.0)  # rain + surplus snowwater\n\n\n\nSnowmelt and refreezing rates as a function of temperature (for set melting and refreezing factors)\n\n\n\n\n\n\nGlacier processes can be modelled if the snow model is enabled. Glacier modelling is very similar to snow modelling and considers two main processes: glacier build-up from snow turning into firn/ice (using the HBV-light model) and glacier melt (using a temperature degree-day model).\nThe definition of glacier boundaries and initial volume is defined by two parameters. The parameter glacierfrac gives the fraction of each grid cell covered by a glacier as a number between zero and one. The state parameter glacierstore gives the amount of water (in mm w.e.) within the glaciers at each grid cell. Because the glacier store (glacierstore) cannot be initialized by running thFe model for a couple of years, a default initial state should be supplied by adding this parameter to the input static file. The required glacier data can be prepared from available glacier datasets.\nFirst, a fixed fraction of the snowpack on top of the glacier is converted into ice for each timestep and added to the glacierstore using the HBV-light model (Seibert et al., 2018). This fraction g_sifrac typically ranges from \\(0.001\\) to \\(0.006\\).\nThen, when the snowpack on top of the glacier is almost all melted (snow cover \\(&lt;\n\\SI{10}{mm}\\)), glacier melt is enabled and estimated with a degree-day model. If the air temperature, \\(T_a\\), is below a certain threshold g_tt (\\(\\SIb{}{\\degree C}\\)) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥\\) g_tt.\nWith this the rate of glacier melt in mm is estimated as:\n\\[\nQ_m = \\subtext{g}{cfmax}(T_a − \\subtext{g}{tt})\\, ; \\, T_a &gt; \\subtext{g}{tt}\n\\]\nwhere \\(Q_m\\) is the rate of glacier melt and \\(\\SIb{\\subtext{g}{cfmax}}{mm (\\degree\nC)^{-1}day^{-1}}\\) is the melting factor. Parameter g_tt can be taken as equal to the snow tt parameter. Values of the melting factor g_cfmax normally varies from one glacier to another and some values are reported in the literature. g_cfmax can also be estimated by multiplying snow cfmax by a factor between 1 and 2, to take into account the higher albedo of ice compared to snow.",
+    "text": "If the air temperature, \\(T_a\\), is below a user-defined threshold tt \\(\\SIb{}{\\degree C}\\) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥ \\mathrm{tt}\\). Another parameter tti defines how precipitation can occur partly as rain or snowfall.\n\n\n\nDivision between snow and precipitation based on the threshold temperature\n\n\n\nIf precipitation occurs as snowfall, it is added to the dry snow component within the snow pack. Otherwise it ends up in the free water reservoir, which represents the liquid water content of the snow pack. Between the two components of the snow pack, interactions take place, either through snow melt (if temperatures are above a threshold tt) or through snow refreezing (if temperatures are below threshold tt).\nThe respective rates of snow melt and refreezing are:\n\\[\n\\begin{align*}\n    Q_m &=& \\subtext{\\mathrm{cf}}{max}(T_a−\\mathrm{tt})\\, &&T_a &gt; \\mathrm{tt} \\\\\n    Q_r &=& \\subtext{\\mathrm{cf}}{max} \\, \\mathrm{cf}_r(\\mathrm{tt}−T_a) &&T_a &lt; \\mathrm{tt}\n\\end{align*}\n\\]\nwhere \\(Q_m\\) is the rate of snow melt, \\(Q_r\\) is the rate of snow refreezing, and \\(\\SIb{\\subtext{\\mathrm{cf}}{max}}{mm\\;(\\degree C)^{-1} day^{-1}}\\) and \\(\\mathrm{cf}_r\\) are user defined model parameters (the melting factor and the refreezing factor respectively).\nThe fraction of liquid water in the snow pack is at most equal to a user defined fraction, whc, of the water equivalent of the dry snow content. If the liquid water concentration exceeds whc, either through snow melt or incoming rainfall, the surplus water (rainfall) becomes available for infiltration into the soil:\nsnowwater = snowwater - refreezing  # free water content in snow\nmaxsnowwater = snow * whc  # max water in the snow\nsnowwater = snowwater + snowmelt + rainfall  # add all water and potentially supersaturate the snowpack\nrainfall = max(snowwater - maxsnowwater, 0.0)  # rain + surplus snowwater\n\n\n\nSnowmelt and refreezing rates as a function of temperature (for set melting and refreezing factors)\n\n\n\n\n\n\nGlacier processes can be modelled if the snow model is enabled. Glacier modelling is very similar to snow modelling and considers two main processes: glacier build-up from snow turning into firn/ice (using the HBV-light model) and glacier melt (using a temperature degree-day model).\nThe definition of glacier boundaries and initial volume is defined by two parameters. The parameter glacierfrac gives the fraction of each grid cell covered by a glacier as a number between zero and one. The state parameter glacierstore gives the amount of water (in mm w.e.) within the glaciers at each grid cell. Because the glacier store (glacierstore) cannot be initialized by running thFe model for a couple of years, a default initial state should be supplied by adding this parameter to the input static file. The required glacier data can be prepared from available glacier datasets.\nFirst, a fixed fraction of the snowpack on top of the glacier is converted into ice for each timestep and added to the glacierstore using the HBV-light model (Seibert et al., 2018). This fraction g_sifrac typically ranges from \\(0.001\\) to \\(0.006\\).\nThen, when the snowpack on top of the glacier is almost all melted (snow cover \\(&lt;\n\\SI{10}{mm}\\)), glacier melt is enabled and estimated with a degree-day model. If the air temperature, \\(T_a\\), is below a certain threshold g_tt (\\(\\SIb{}{\\degree C}\\)) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥\\) g_tt.\nWith this the rate of glacier melt in mm is estimated as:\n\\[\nQ_m = \\subtext{g}{cfmax}(T_a − \\subtext{g}{tt})\\, ; \\, T_a &gt; \\subtext{g}{tt}\n\\]\nwhere \\(Q_m\\) is the rate of glacier melt and \\(\\SIb{\\subtext{g}{cfmax}}{mm (\\degree\nC)^{-1}day^{-1}}\\) is the melting factor. Parameter g_tt can be taken as equal to the snow tt parameter. Values of the melting factor g_cfmax normally varies from one glacier to another and some values are reported in the literature. g_cfmax can also be estimated by multiplying snow cfmax by a factor between 1 and 2, to take into account the higher albedo of ice compared to snow.",
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@@ -1353,7 +1353,7 @@
     "href": "model_docs/vertical/shared_processes.html#snow-and-glaciers",
     "title": "Shared processes",
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-    "text": "If the air temperature, \\(T_a\\), is below a user-defined threshold tt \\(\\SIb{}{\\degree C}\\) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥ \\mathrm{tt}\\). A another parameter tti defines how precipitation can occur partly as rain or snowfall.\n\n\n\nDivision between snow and precipitation based on the threshold temperature\n\n\n\nIf precipitation occurs as snowfall, it is added to the dry snow component within the snow pack. Otherwise it ends up in the free water reservoir, which represents the liquid water content of the snow pack. Between the two components of the snow pack, interactions take place, either through snow melt (if temperatures are above a threshold tt) or through snow refreezing (if temperatures are below threshold tt).\nThe respective rates of snow melt and refreezing are:\n\\[\n\\begin{align*}\n    Q_m &=& \\subtext{\\mathrm{cf}}{max}(T_a−\\mathrm{tt})\\, &&T_a &gt; \\mathrm{tt} \\\\\n    Q_r &=& \\subtext{\\mathrm{cf}}{max} \\, \\mathrm{cf}_r(\\mathrm{tt}−T_a) &&T_a &lt; \\mathrm{tt}\n\\end{align*}\n\\]\nwhere \\(Q_m\\) is the rate of snow melt, \\(Q_r\\) is the rate of snow refreezing, and \\(\\SIb{\\subtext{\\mathrm{cf}}{max}}{mm\\;(\\degree C)^{-1} day^{-1}}\\) and \\(\\mathrm{cf}_r\\) are user defined model parameters (the melting factor and the refreezing factor respectively).\nThe fraction of liquid water in the snow pack is at most equal to a user defined fraction, whc, of the water equivalent of the dry snow content. If the liquid water concentration exceeds whc, either through snow melt or incoming rainfall, the surplus water (rainfall) becomes available for infiltration into the soil:\nsnowwater = snowwater - refreezing  # free water content in snow\nmaxsnowwater = snow * whc  # max water in the snow\nsnowwater = snowwater + snowmelt + rainfall  # add all water and potentially supersaturate the snowpack\nrainfall = max(snowwater - maxsnowwater, 0.0)  # rain + surplus snowwater\n\n\n\nSnowmelt and refreezing rates as a function of temperature (for set melting and refreezing factors)\n\n\n\n\n\n\nGlacier processes can be modelled if the snow model is enabled. Glacier modelling is very similar to snow modelling and considers two main processes: glacier build-up from snow turning into firn/ice (using the HBV-light model) and glacier melt (using a temperature degree-day model).\nThe definition of glacier boundaries and initial volume is defined by two parameters. The parameter glacierfrac gives the fraction of each grid cell covered by a glacier as a number between zero and one. The state parameter glacierstore gives the amount of water (in mm w.e.) within the glaciers at each grid cell. Because the glacier store (glacierstore) cannot be initialized by running thFe model for a couple of years, a default initial state should be supplied by adding this parameter to the input static file. The required glacier data can be prepared from available glacier datasets.\nFirst, a fixed fraction of the snowpack on top of the glacier is converted into ice for each timestep and added to the glacierstore using the HBV-light model (Seibert et al., 2018). This fraction g_sifrac typically ranges from \\(0.001\\) to \\(0.006\\).\nThen, when the snowpack on top of the glacier is almost all melted (snow cover \\(&lt;\n\\SI{10}{mm}\\)), glacier melt is enabled and estimated with a degree-day model. If the air temperature, \\(T_a\\), is below a certain threshold g_tt (\\(\\SIb{}{\\degree C}\\)) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥\\) g_tt.\nWith this the rate of glacier melt in mm is estimated as:\n\\[\nQ_m = \\subtext{g}{cfmax}(T_a − \\subtext{g}{tt})\\, ; \\, T_a &gt; \\subtext{g}{tt}\n\\]\nwhere \\(Q_m\\) is the rate of glacier melt and \\(\\SIb{\\subtext{g}{cfmax}}{mm (\\degree\nC)^{-1}day^{-1}}\\) is the melting factor. Parameter g_tt can be taken as equal to the snow tt parameter. Values of the melting factor g_cfmax normally varies from one glacier to another and some values are reported in the literature. g_cfmax can also be estimated by multiplying snow cfmax by a factor between 1 and 2, to take into account the higher albedo of ice compared to snow.",
+    "text": "If the air temperature, \\(T_a\\), is below a user-defined threshold tt \\(\\SIb{}{\\degree C}\\) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥ \\mathrm{tt}\\). Another parameter tti defines how precipitation can occur partly as rain or snowfall.\n\n\n\nDivision between snow and precipitation based on the threshold temperature\n\n\n\nIf precipitation occurs as snowfall, it is added to the dry snow component within the snow pack. Otherwise it ends up in the free water reservoir, which represents the liquid water content of the snow pack. Between the two components of the snow pack, interactions take place, either through snow melt (if temperatures are above a threshold tt) or through snow refreezing (if temperatures are below threshold tt).\nThe respective rates of snow melt and refreezing are:\n\\[\n\\begin{align*}\n    Q_m &=& \\subtext{\\mathrm{cf}}{max}(T_a−\\mathrm{tt})\\, &&T_a &gt; \\mathrm{tt} \\\\\n    Q_r &=& \\subtext{\\mathrm{cf}}{max} \\, \\mathrm{cf}_r(\\mathrm{tt}−T_a) &&T_a &lt; \\mathrm{tt}\n\\end{align*}\n\\]\nwhere \\(Q_m\\) is the rate of snow melt, \\(Q_r\\) is the rate of snow refreezing, and \\(\\SIb{\\subtext{\\mathrm{cf}}{max}}{mm\\;(\\degree C)^{-1} day^{-1}}\\) and \\(\\mathrm{cf}_r\\) are user defined model parameters (the melting factor and the refreezing factor respectively).\nThe fraction of liquid water in the snow pack is at most equal to a user defined fraction, whc, of the water equivalent of the dry snow content. If the liquid water concentration exceeds whc, either through snow melt or incoming rainfall, the surplus water (rainfall) becomes available for infiltration into the soil:\nsnowwater = snowwater - refreezing  # free water content in snow\nmaxsnowwater = snow * whc  # max water in the snow\nsnowwater = snowwater + snowmelt + rainfall  # add all water and potentially supersaturate the snowpack\nrainfall = max(snowwater - maxsnowwater, 0.0)  # rain + surplus snowwater\n\n\n\nSnowmelt and refreezing rates as a function of temperature (for set melting and refreezing factors)\n\n\n\n\n\n\nGlacier processes can be modelled if the snow model is enabled. Glacier modelling is very similar to snow modelling and considers two main processes: glacier build-up from snow turning into firn/ice (using the HBV-light model) and glacier melt (using a temperature degree-day model).\nThe definition of glacier boundaries and initial volume is defined by two parameters. The parameter glacierfrac gives the fraction of each grid cell covered by a glacier as a number between zero and one. The state parameter glacierstore gives the amount of water (in mm w.e.) within the glaciers at each grid cell. Because the glacier store (glacierstore) cannot be initialized by running thFe model for a couple of years, a default initial state should be supplied by adding this parameter to the input static file. The required glacier data can be prepared from available glacier datasets.\nFirst, a fixed fraction of the snowpack on top of the glacier is converted into ice for each timestep and added to the glacierstore using the HBV-light model (Seibert et al., 2018). This fraction g_sifrac typically ranges from \\(0.001\\) to \\(0.006\\).\nThen, when the snowpack on top of the glacier is almost all melted (snow cover \\(&lt;\n\\SI{10}{mm}\\)), glacier melt is enabled and estimated with a degree-day model. If the air temperature, \\(T_a\\), is below a certain threshold g_tt (\\(\\SIb{}{\\degree C}\\)) precipitation occurs as snowfall, whereas it occurs as rainfall if \\(T_a ≥\\) g_tt.\nWith this the rate of glacier melt in mm is estimated as:\n\\[\nQ_m = \\subtext{g}{cfmax}(T_a − \\subtext{g}{tt})\\, ; \\, T_a &gt; \\subtext{g}{tt}\n\\]\nwhere \\(Q_m\\) is the rate of glacier melt and \\(\\SIb{\\subtext{g}{cfmax}}{mm (\\degree\nC)^{-1}day^{-1}}\\) is the melting factor. Parameter g_tt can be taken as equal to the snow tt parameter. Values of the melting factor g_cfmax normally varies from one glacier to another and some values are reported in the literature. g_cfmax can also be estimated by multiplying snow cfmax by a factor between 1 and 2, to take into account the higher albedo of ice compared to snow.",
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