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start:hype_model_description:hype_tracer [2018/10/11 17:43]
cpers [Lake and river ice]
start:hype_model_description:hype_tracer [2024/01/25 11:37] (current)
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 |Simulated amount T1 in or above soil (//aT11//, //aT12//, //aT13//, //sT11//, //sT12//, //sT13//, //​T1sf//​)|U/​km2|kg/​km2|#/​km2| |Simulated amount T1 in or above soil (//aT11//, //aT12//, //aT13//, //sT11//, //sT12//, //sT13//, //​T1sf//​)|U/​km2|kg/​km2|#/​km2|
 |Simulated amount T1 in river sediment (//Tsmr//, //​Tslr//​)|U|kg|#​| |Simulated amount T1 in river sediment (//Tsmr//, //​Tslr//​)|U|kg|#​|
 +|Simulated sedimenting amount T1 in outlet lake (//​ola1//​)|U|kg|#​|
 |Simulated concentration of water (//coT1//, //ceT1//, //csT1//, //ccT1//, //clT1//, //Tcr1//, //Tcr2//, //Tcr3//, //Tcrd//, //​Tcrs//​)|mU/​m3 or µU/​L|mg/​L|thousandth part/m3 or millionth part/L| |Simulated concentration of water (//coT1//, //ceT1//, //csT1//, //ccT1//, //clT1//, //Tcr1//, //Tcr2//, //Tcr3//, //Tcrd//, //​Tcrs//​)|mU/​m3 or µU/​L|mg/​L|thousandth part/m3 or millionth part/L|
 |Observed concentration (//​reT1//​)|mU/​m3 or µU/​L|mg/​L|thousandth part/m3 or millionth part/L| |Observed concentration (//​reT1//​)|mU/​m3 or µU/​L|mg/​L|thousandth part/m3 or millionth part/L|
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 2) Point sources may be a source of T1 to surface waters. Point sources of tracer T1 can be added to the local stream, the local lake, the main river or the outlet lake. 2) Point sources may be a source of T1 to surface waters. Point sources of tracer T1 can be added to the local stream, the local lake, the main river or the outlet lake.
  
-3) A pool laid down on land can be a source of the tracer. ​The pool is defined ​similar to the manure for nutrients ​(//​t1amount//​). It can be added at a specific point in time or equally distributed over a period of time. The pool may be tilled down into the top soil layers ​also in similar fashion as manure.+3) A pool laid down on land can be a source of the tracer. ​This source (//​tamount//​) ​is a bit similar to the handling of the source of manure for nutrients. It can be added at a specific point in time or equally distributed over a period of time. Part of the pool may be tilled down into the top soil layer or the top two layers.
  
 4) The tracer can be introduced to HYPE in the form of typical concentrations for leakage from different land-uses and/or soil types. The concentration of the runoff from a class (//conc//) is calculated as the product of two model parameters: ​ 4) The tracer can be introduced to HYPE in the form of typical concentrations for leakage from different land-uses and/or soil types. The concentration of the runoff from a class (//conc//) is calculated as the product of two model parameters: ​
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 === Release from above ground storage === === Release from above ground storage ===
-T1 can be released from storage above ground (e.g. manure) by rain and snowmelt (flow //q// (mm/day)). The released tracer will follow the flow, as a concentration,​ and depending on the fate of the flow, the tracer may follow surface runoff, infiltration or other path ways. The release is goverened by the model parameter //t1rel// (1/mm). A fraction (<​m>​a_rel</​m>​) of the total amount of tracer in the store above ground is released ​and follows the flow according to equation:+T1 is released from the storage above ground (e.g. manure) by rain and snowmelt (flow //q// (mm/day)). The release is goverened by the model parameter //t1rel// (1/mm). A fraction (<​m>​a_rel</​m>​) of the total amount of tracer in the store above ground is released according to equation:
  
 <m> a_rel = 1-e^{-t1rel*q} </m> <m> a_rel = 1-e^{-t1rel*q} </m>
 +
 +The released tracer will follow the surface flow or the infiltration flow. If there is surface flow (saturated overland flow or infiltration excess surface flow) a part will follow that flow as a concentration. If there is infiltration,​ a part will infiltrate into the top soil layer where it will be adsorbed. The division is determined by the relative sizes of surface flow and tinfiltration flow. 
  
 === Exponential decay === === Exponential decay ===
-Patogens grow and die over time. To simulate this, HYPE supplies a process for the combined effect as an exponential decay. The process is goverened by the model paramater //​t1expdec//,​ which denote the halv life time of the tracer in days. Exponential decay is applied to tracer T1 in most forms; in soil water, river, lakes, the above ground storage, tracers adsorbed to soil and tracers in river sediment.+Patogens grow and die over time. To simulate this, HYPE supplies a process for the combined effect as an exponential decay. The process is goverened by the model paramater //​t1expdec//,​ which denote the half-life of the tracer in days. Exponential decay is applied to tracer T1 in most forms; in soil water, river, lakes, the above ground storage, tracers adsorbed to soil and tracers in river sediment.
  
 === Adsorption/​desorption === === Adsorption/​desorption ===
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 === Sedimentation/​resuspension in river === === Sedimentation/​resuspension in river ===
-Sedimentation or resuspension of tracers in rivers is calculated the same way as particulate phosphorus (described [[start:​hype_model_description:​hype_np_riv_lake#​sedimentation_resuspension|here]]). ​The process depends on the current flow (//q//) in the river in relation to bankful flow (<​m>​q_bank</​m>​) and the general model parameter //​t1sedexp//​. Bankful flow is the flow when the river is filled to the brim. This flow is calculated as the second largest simulated flow in the last year. The fraction of the tracer that is resuspended or sedimented is determined by the equation:+Sedimentation or resuspension of tracers in rivers is calculated the same way as particulate phosphorus (described [[start:​hype_model_description:​hype_np_riv_lake#​sedimentation_resuspension|here]]) and suspended sediments (described [[start:​hype_model_description:​hype_sediment#​sedimentation_resuspension_in_rivers|here]]). ​There are two alternative models. For the original the process depends on the current flow (//q//) in the river in relation to an reduced ​bankful flow (<​m>​q_bank</​m>​) and the general model parameter //​t1sedexp//​. Bankful flow is the flow when the river is filled to the brim. This flow is calculated as the second largest simulated flow in the last year. It has been adjusted with the value 0.7 or by the parameter //qbank//. The fraction of the tracer that is resuspended or sedimented is determined by the equation:
  
 <m> a_sres=max(-1.,​min(1.,​{{q_bank-q}/​q_bank}^{t1sedexp}-{q/​q_bank}^{t1sedexp})) </m> <m> a_sres=max(-1.,​min(1.,​{{q_bank-q}/​q_bank}^{t1sedexp}-{q/​q_bank}^{t1sedexp})) </m>
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 where <​m>​c_river</​m>​ is the concentration of T1 in river (U/m3), <​m>​v_river</​m>​ is the volume of river (m3), and //Ased// is amount of tracer T1 in the sediment (U).  where <​m>​c_river</​m>​ is the concentration of T1 in river (U/m3), <​m>​v_river</​m>​ is the volume of river (m3), and //Ased// is amount of tracer T1 in the sediment (U). 
 +
 +An alternative model is the Bagnold equation (see sediment). The tracer sedimentation/​resuspension with this model uses T1 specific parameters to calculate the maximum suspended T1 concentration in the river, general parameters //​suspconT1//​ and //​suspexpT1//​.
  
 === Sedimentation in lakes === === Sedimentation in lakes ===
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 |Sources| |//​cpt1//​|[[start:​hype_file_reference:​xobs.txt|Xobs.txt]]| |Sources| |//​cpt1//​|[[start:​hype_file_reference:​xobs.txt|Xobs.txt]]|
 |:::| |//​ps_t1//​|[[start:​hype_file_reference:​pointsourcedata.txt|PointSourceData.txt]]| |:::| |//​ps_t1//​|[[start:​hype_file_reference:​pointsourcedata.txt|PointSourceData.txt]]|
-|:::| |//t1amount//​|[[start:​hype_file_reference:​cropdata.txt|CropData.txt]]|+|:::| |//tamount//​|[[start:​hype_file_reference:​cropdata.txt|CropData.txt]]|
 |:::​|//​t1leakluse,​ t1leaksoil//​|//​t1leakluse,​ t1leaksoil//​|[[start:​hype_file_reference:​par.txt|par.txt]]| |:::​|//​t1leakluse,​ t1leaksoil//​|//​t1leakluse,​ t1leaksoil//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 |Processes|//​t1rel,​ t1sedexp, t1freuc//​|//​t1rel,​ t1sedexp, t1freuc//​|[[start:​hype_file_reference:​par.txt|par.txt]]| |Processes|//​t1rel,​ t1sedexp, t1freuc//​|//​t1rel,​ t1sedexp, t1freuc//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
-|:::| |//t1evap, t1expdec, t1sedvel//​|:::​|+|:::| |//t1evap, t1expdec, t1sedvel, qbank, suspcont1, suspexpt1//|:::|
 |:::|//d//| |[[start:​hype_file_reference:​geoclass.txt|GeoClass.txt]]| |:::|//d//| |[[start:​hype_file_reference:​geoclass.txt|GeoClass.txt]]|
  
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 ^Modules (file) ^Procedures ^ ^Modules (file) ^Procedures ^
-|[[http://​hype.sourceforge.net/​doxy-html/​classtracer__processes.html|tracer_processes (t_proc.f90)]]|add_tracer_point_source_to_river|+|[[http://​hype.sourceforge.net/​doxy-html/​namespacetracer__processes.html|tracer_processes (t_proc.f90)]]|add_tracer_point_source_to_river|
 | ::: |add_tracer_point_source_to_lake| | ::: |add_tracer_point_source_to_lake|
 | ::: |soil_tracer_processes| | ::: |soil_tracer_processes|
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 === Black ice growth === === Black ice growth ===
  
-Black ice growth (<​m>​dH_i/​dt</​m>​ (cm/s)) is derived from the modified Stefan’s equations as described by Leppäranta (1983):+Black ice growth (<​m>​dH_i/​dt</​m>​ (cm/s)) is derived from the modified Stefan’s equations as described by Leppäranta (1983) ​reduced by heat flow from water.
  
-<m> dH_i/dt = {k_i/{rho_i * L_f}}*{(T_f - T_a)/​(H_i+H_s*{k_i/​k_s}+k_i/​k_a)} </m>+<m> dH_i/dt = {k_i/{rho_i * L_f}}*{(T_f - T_a)/​(H_i+H_s*{k_i/​k_s}+k_i/​k_a)}- qh*100/​rho_i/​T_f ​</m>
  
 The first part is constant in HYPE. //​k<​sub>​i</​sub>//​ is thermal conductivity of ice (0.022 J/​°C/​cm/​s),​ //​ρ<​sub>​i</​sub>//​ is density of ice (0.917 g/​cm<​sup>​3</​sup>​),​ and //​L<​sub>​f</​sub>//​ is latent heat of freezing (334 J/g). The first part is constant in HYPE. //​k<​sub>​i</​sub>//​ is thermal conductivity of ice (0.022 J/​°C/​cm/​s),​ //​ρ<​sub>​i</​sub>//​ is density of ice (0.917 g/​cm<​sup>​3</​sup>​),​ and //​L<​sub>​f</​sub>//​ is latent heat of freezing (334 J/g).
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 where //​ρ<​sub>​s</​sub>//​ is density of snow (g/​cm<​sup>​3</​sup>​). Snow density changes over time depending on a change parameter (//​sndens//​). where //​ρ<​sub>​s</​sub>//​ is density of snow (g/​cm<​sup>​3</​sup>​). Snow density changes over time depending on a change parameter (//​sndens//​).
 +
 +//qh// is heat flow from water during the time step (MJ/​m2/​day). For rivers it is calculated depending on river velocity (//vel//) and depth (Hw), but for lake it is constant, (parameter //​liceqhw//,​ W/m2). The river equation is 
 +
 +<m> qh = (T_w-T_f)*{{Cwi*vel^0.8}/​{Hw^0.2}} * unitf </m>
 +
 +but limited by minimum and maximum parameters (//​riceqhmn,​ riceqhmx//​). //​T<​sub>​w</​sub>//​ is water temperature,​ //Cwi// is the heat exchange coefficient,​ a parameter. A unit transformation (//unitf//) is made from W/m2 to MJ/m2/day.
 +
  
 The heat released when the black ice is formed at the bottom of the ice layer (<​m>​rho_i * L_f * {dH_i/​dt}</​m>​) is conducted through the ice and the overlaying snow layer to the atmosphere. This heat flow is driven by the temperature gradient between the air above the ice or snow surface and the freezing temperature of the water assumed at the bottom of the ice layer, and is governed by the depths and thermal conductivities in the ice and snow layers, and the heat exchange coefficient in the air. It should also be noted that a term representing the heat flow from the water has been neglected compared to Leppäranta (1983). ​ The heat released when the black ice is formed at the bottom of the ice layer (<​m>​rho_i * L_f * {dH_i/​dt}</​m>​) is conducted through the ice and the overlaying snow layer to the atmosphere. This heat flow is driven by the temperature gradient between the air above the ice or snow surface and the freezing temperature of the water assumed at the bottom of the ice layer, and is governed by the depths and thermal conductivities in the ice and snow layers, and the heat exchange coefficient in the air. It should also be noted that a term representing the heat flow from the water has been neglected compared to Leppäranta (1983). ​
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 Snow and ice melt is calculated with a simple temperature index model when air temperature is above 0°C. The snow on the ice has to be completely melted before any ice melt is calculated: Snow and ice melt is calculated with a simple temperature index model when air temperature is above 0°C. The snow on the ice has to be completely melted before any ice melt is calculated:
  
-<m> dH_i/dt=-p_m * T_a </m>+<m> dH_i/dt=-p_mt * T_a </m>
  
-Ice can be melted ​from below if the water contain enough heatThis process ​is limited by melt efficiency parameter ​(//meff//).+Ice can in addition ​be melted ​internally by radiation. 
 + 
 +<m> dH_i/​dt=-{p_mr *100} / {L_f * rho_i} </​m>​ 
 + 
 +Final ice break-up ​is defined as the time step when either the ice thickness is zero or the ice porosity is less than threshold. The thresholds are given by general parameters; different for river and lakes (//ricebupo, licebupo//).
  
-Final ice break-up is defined as the time step when //​H<​sub>​i</​sub>//​=0. Although it is well known that ice tend to fall apart before it is completely melted, this is not considered by the present model. ​ 
  
 === Initiation of ice growth === === Initiation of ice growth ===
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 ==== Surface water processes ==== ==== Surface water processes ====
  
-Temperature T2 of a river is not affected by irrigation withdrawal, abstractions,​ rural households or point source additions, constructed wetlands, or water returning from aquifers. ​+=== River model option === 
 + 
 +As default, temperature of the main river flow is affected by the temperature of water added to the river. ​Temperature T2 of a river is not affected by point sources which not have T2 (''​ps_t2''​) set in PointSourceData though. In this case the recieving main river flow will keep the temperature it had before adding of the point sources. 
 + 
 +In earlier HYPE versions, the temperature of the river was not affected by irrigation withdrawal, abstractions,​ rural households or point source additions, constructed wetlands, or water returning from aquifers. ​To get this older function of T2 in HYPE, there is a modeloption that can be set (modeloption rivert2model 1). 
  
 === Lake basic assumptions === === Lake basic assumptions ===
  
-For substances the lake volume is divided into two parts FLP and SLP (see Chapter [[start:​hype_model_description:​hype_routing#​basic_assumptions|Rivers and lakes - Basic assumptions]])). In addition to simulating ​temperature as the substance T2 in the two lake parts, ​states of lake temperature in a hypothetical epilimnion and hypolimnion (//​uppertemp//,​ //​lowertemp//​) is handled in the model. The average temperature of FLP+SLP ​is equal to the average temp of the EPI+HYPO. The size of volumes related to the upper and lower temperatures are determined by the thermocline which is estimated for each olake.+To simulate ​temperature as the substance T2 the lake is divided ​in two lake parts, lake temperature in a hypothetical epilimnion and hypolimnion (//​uppertemp//,​ //​lowertemp//​) is handled in the model. The average temperature of the lake is also a state variable. The size of volumes related to the upper and lower temperatures are determined by the thermocline which is estimated for each outlet lake.
  
-|{{:​start:​hype_model_description:​two_divisions_of_lake.png?500|}}| +| {{:​start:​hype_model_description:​epi_hypo_lake.png?400}}                 ​
-|Figure 3: Two different divisions ​of a lake. Left: two parts signifying fast flows (FLP) and slow flows (SLP). Right: epilimnion (EPI) and hypolimnion (HYPO).|+| Figure 3: Division ​of a lake: epilimnion (EPI) and hypolimnion (HYPO). ​ |
  
 Thermocline depth is estimated from lake area (Hanna, 1990). This average depth is adjusted for current changes by adding precipitation (//prec//) and inflow (//qin//) to the lake, and remove evaporation (//​evap//​). ​ Thermocline depth is estimated from lake area (Hanna, 1990). This average depth is adjusted for current changes by adding precipitation (//prec//) and inflow (//qin//) to the lake, and remove evaporation (//​evap//​). ​
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 === Evaporation === === Evaporation ===
  
-Lakes and rivers with given class area may have evaporation. The actual evaporating area is reduced if it is ice covered. Evaporation is not changing the T2 temperature of the river or lake. The latent heat is assumed to be taken care of by the water - atmosphere T2 exchange routine. River evaporation is removed proportionally from the water stores making up the river volume. Lake evaporation may be removed from one or both lake parts (FLP and SLP).+Lakes and rivers with given class area may have evaporation. The actual evaporating area is reduced if it is ice covered. Evaporation is not changing the T2 temperature of the river or lake. The latent heat is assumed to be taken care of by the water - atmosphere T2 exchange routine. River evaporation is removed proportionally from the water stores making up the river volume.
  
 Evaporation from flooded floodplain of rivers or lakes also keep the temperature of the flooded water unchanged. Evaporation from flooded floodplain of rivers or lakes also keep the temperature of the flooded water unchanged.
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 === Lake outflow === === Lake outflow ===
  
-Lake outflow T2 temperature may be determined by the T2 of the lake parts (FLP and SLP) contributing to outflow (see Figure 2). To use this method set parameter //t2mix//. For ilakes the t2mix method is always used. +Lake outflow T2 temperature may be determined by the average ​T2 of the lake. To use this method set parameter //t2mix//. For ilakes the t2mix method is always used. 
  
 For outlet lakes another method for determining lake outflow temperature is the default method. This method assigns uppertemp to outflow water if the lake is stratified and the thermocline is deeper than the lake threshold (//​thres//​). For other conditions a mixture of upper and lowertemp is used to set the outflow temperature (//​t2out//​). For outlet lakes another method for determining lake outflow temperature is the default method. This method assigns uppertemp to outflow water if the lake is stratified and the thermocline is deeper than the lake threshold (//​thres//​). For other conditions a mixture of upper and lowertemp is used to set the outflow temperature (//​t2out//​).
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 |:::​|<​m>​k_exp</​m>​|//​ricekexp,​ licekexp//​|:::​| |:::​|<​m>​k_exp</​m>​|//​ricekexp,​ licekexp//​|:::​|
 |:::​|//​sndens//​|//​ricesndens,​ licesndens//​|:::​| |:::​|//​sndens//​|//​ricesndens,​ licesndens//​|:::​|
-|:::​|<​m>​p_m</​m>​|//​ricetmelt,​ licetmelt//​|:::​|+|:::​|<​m>​p_mt</​m>​|//​ricetmelt,​ licetmelt//|:::| 
 +|:::​|<​m>​p_mr</​m>​|//​ricermelt,​ licermelt//|:::|
 |:::​|//​meff//​|//​ricewme,​ licewme//​|:::​| |:::​|//​meff//​|//​ricewme,​ licewme//​|:::​|
 +|:::|//vel, Cwi//​|//​rivvel,​ ricecwi//​|:::​|
 +|:::| |//​riceqhmn,​ riceqhmx, liceqhw, ricebupo, licebupo//​|:::​|
 |Surface water processes|//​tcf//​|//​tcfriver,​ tcflake//​|[[start:​hype_file_reference:​par.txt|par.txt]]| |Surface water processes|//​tcf//​|//​tcfriver,​ tcflake//​|[[start:​hype_file_reference:​par.txt|par.txt]]|
 |:::​|//​scf//​|//​scfriver,​ scflake//​|:::​| |:::​|//​scf//​|//​scfriver,​ scflake//​|:::​|
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 ^Modules (file) ^Procedures ^Section^ ^Modules (file) ^Procedures ^Section^
-|[[http://​hype.sourceforge.net/​doxy-html/​classtracer__processes.html|tracer_processes (t_proc.f90)]]|add_tracer_point_source_to_river|point source|+|[[http://​hype.sourceforge.net/​doxy-html/​namespacetracer__processes.html|tracer_processes (t_proc.f90)]]|add_tracer_point_source_to_river|point source|
 | ::: |add_tracer_point_source_to_lake| ::: | | ::: |add_tracer_point_source_to_lake| ::: |
-|[[http://​hype.sourceforge.net/​doxy-html/​classnpc_surfacewater__processes.html|npc_surfacewater_processes (npc_sw_proc.f90)]]|add_point_sources_to_main_river| ::: | +|[[http://​hype.sourceforge.net/​doxy-html/​namespacenpc__surfacewater__processes.html|npc_surfacewater_processes (npc_sw_proc.f90)]]|add_point_sources_to_main_river| ::: | 
-|[[http://​hype.sourceforge.net/​doxy-html/​classnpc_soil__processes.html|npc_soil_processes (npc_soil_proc.f90)]]|set_class_precipitation_concentration_and_load|precipitation| +|[[http://​hype.sourceforge.net/​doxy-html/​namespacenpc__soil__processes.html|npc_soil_processes (npc_soil_proc.f90)]]|set_class_precipitation_concentration_and_load|precipitation| 
-|[[http://​hype.sourceforge.net/​doxy-html/​classsurfacewater__processes.html|surfacewater_processes (sw_proc.f90)]]|add_T2_concentration_in_precipitation_on_water|:::​|+|[[http://​hype.sourceforge.net/​doxy-html/​namespacesurfacewater__processes.html|surfacewater_processes (sw_proc.f90)]]|add_T2_concentration_in_precipitation_on_water|:::​|
 | ::: |calculate_river_evaporation|evaporation| | ::: |calculate_river_evaporation|evaporation|
 | ::: |calculate_lake_epilimnion_depth|lake basic assumptions| | ::: |calculate_lake_epilimnion_depth|lake basic assumptions|
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 |:::​|riverice_riverwater_interaction|:::​| |:::​|riverice_riverwater_interaction|:::​|
 |:::​|calculate_lakeice_lakewater_interaction|:::​| |:::​|calculate_lakeice_lakewater_interaction|:::​|
-|[[http://​hype.sourceforge.net/​doxy-html/​classsoil__processes.html|soil_processes (soil_proc.f90)]]|calculate_snowmelt|:::​|+|[[http://​hype.sourceforge.net/​doxy-html/​namespacesoil__processes.html|soil_processes (soil_proc.f90)]]|calculate_snowmelt|:::​|
 |:::​|calculate_snowdepth|:::​| |:::​|calculate_snowdepth|:::​|
 |:::​|calculate_snow|sources| |:::​|calculate_snow|sources|
-|[[http://​hype.sourceforge.net/​doxy-html/​classregional__groundwater.html|regional_groundwater (regional_groundwater.f90)]]|initiate_aquifer_state|| +|[[http://​hype.sourceforge.net/​doxy-html/​namespaceregional__groundwater__module.html|regional_groundwater (regional_groundwater.f90)]]|initiate_aquifer_state|| 
-|[[http://​hype.sourceforge.net/​doxy-html/​classsoilmodel__default.html|soilmodel_default (soilmodel0.f90)]]|soilmodel_0|soil temperature and runoff| +|[[http://​hype.sourceforge.net/​doxy-html/​namespacesoilmodel__default.html|soilmodel_default (soilmodel0.f90)]]|soilmodel_0|soil temperature and runoff| 
-|[[http://​hype.sourceforge.net/​doxy-html/​classglacier__soilmodel.html|glacier_soilmodel (glacier_soilmodel.f90)]]|soilmodel_3| ::: | +|[[http://​hype.sourceforge.net/​doxy-html/​namespaceglacier__soilmodel.html|glacier_soilmodel (glacier_soilmodel.f90)]]|soilmodel_3| ::: | 
-|[[http://​hype.sourceforge.net/​doxy-html/​classfloodplain__soilmodel.html|soilmodel_4 (soilmodel4.f90)]]|soilmodel_4| ::: |+|[[http://​hype.sourceforge.net/​doxy-html/​namespacefloodplain__soilmodel.html|soilmodel_4 (soilmodel4.f90)]]|soilmodel_4| ::: |
  
start/hype_model_description/hype_tracer.1539272598.txt.gz · Last modified: 2023/11/16 14:28 (external edit)