Difference between revisions of "Continuous:Snowfall Accumulation and Melting"

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When GSSHA is run in the '''LONG_TERM''' simulation mode, snowfall accumulation and melting is simulated.   Because the CASC2D model has no explicit way to account for the seasonal variability in hydrologic response of watersheds its appropriate use has been limited to periods where seasonal effects can largely be ignored, and has most typically been applied during the summer growing season (Senarath et al., 2000; Downer et al., 2002a).  An energy balance method of estimating snowfall accumulation and melting has been added to the GSSHA model to increase its utility in regions with significant snowfall.  This method is admittedly simple and other factors, soil freezing, change in overland roughness, etc, are not yet considered.  This is an area of active research and model development at ERDC.
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When GSSHA is run in the '''LONG_TERM''' simulation mode, snowfall accumulation and melting is simulated to increase its utility in regions with significant snowfall. More accurate snow accumulation and melt algorithms as well as more accurate melt transport algorithms within GSSHA are active research and model development areas at ERDC.  Snowfall has a large impact on hydrologic fluxes because snowfall is normally stored for a significant period of time in the snowpack and is later released as melt water.  In many parts of the world melt of the snow cover is the single most important event of the water year (Gray and Prowse, 1993). Because snowfall accumulation and subsequent melting can have such a large influence in hydrologic response of a watershed, it is important to simulate these processes.  The purpose of the snowfall accumulation and melting routine is to allow an accounting of these processes with the intent to differentiate between precipitation that is rainfall that will immediately infiltrate, pond and runoff or evaporate, and snow and ice that accumulates and significantly alters the timing of hydrologic fluxes.
  
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Snowfall has a large impact on hydrologic fluxes because snowfall is normally stored for a significant period of time in the snowpack and is later released as melt water.  In many parts of the world melt of the snow cover is the single most important event of the water year (Gray and Prowse, 1993).  Because snowfall accumulation and subsequent melting can have such a large influence in hydrologic response of a watershed, it is important to simulate these processes.  The purpose of the snowfall accumulation and melting routine is to allow an accounting of these processes with the intent to differentiate between precipitation that is rainfall that will immediately infiltrate, pond and runoff or evaporate, and snow and ice that accumulates and significantly alters the timing of hydrologic fluxes.  Precipitation freezing and snowpack melting can be modeled during long-term simulations when hourly hydrometeorological data values of air temperature (''T<sub>a</sub>''), relative humidity (''r<sub>h</sub>''), wind speed (''U'') barometric pressure (''P<sub>a</sub>'') and cloud cover, are required inputs. 
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All three methods used within GSSHA to simulate snow accumulation and melt assume that the snow pack consists of a single layer.  Certain advantages - such as time variations of liquid water content (Bloschl & Kirnbauer 1991), interflow within the snow pack layers due to ice sheets, and avalanche modeling (Colbeck 1991) - do exist when applying multi-layer snow models, but the required data to accomplish such models on a watershed level is currently unrealistic in most basins.  Multi-layer snow models are typically deployed at the site-scale where spatially-close data is available.<br>
  
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Anytime the air temperature is below 0&deg; C during precipitation, the precipitation is assumed to be snow or ice that will accumulate on the land surface.  At air temperatures below 0&deg; C, precipitation is nearly always snowfall (Gray and Prowse, 1993). If snow is already present in a cell, the new snow accumulation is added to the existing accumulated snow.  While precipitation in the GSSHA model is distributed over the land surface, the effects of vegetation, elevation, and wind on the spatial distribution of snowfall are ignored.
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In nature snow is a distributed process.  Because of the distributed structure of the GSSHA model the snow is modeled as a distributed process.  Utilizing a distributed domain gives more potential of addressing a variety of real world problems than a semi-distributed or lumped-parameter model (kirnbauer, Bloeschl et al. 1994).  Because of the distributed domain, the model can also account for '''[[Orographic Effects]]'''.
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Snowmelt models use either an energy balance or a temperature-index method.  Physically-based systems are recommended for short term forecasts (Gray and Prowse, 1993), which are needed for hydrologic modeling.  In the energy budget model the amount of heat available is applied to the snowpack and the amount of meltwater is calculated.  The simplest representation of the snowpack is used; each 80 calories of heat added to the snowpack results in the release of 1 cm<sup>3</sup> of meltwater (Linsley et al., 1982, Gray and Prowse, 1993).  This method ignores complex snowpack behavior, such as ripening of the snowpack and refreezing of meltwater.  Hourly values of hydrometeorological variables allow both seasonal and diurnal variations in climatic conditions to be included in the heat balance.
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'''GSSHA Melt Algorithms'''<br>
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GSSHA currently employs three snow melt models:
  
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The amount of heat, Q (cal cm<sup>-2</sup> hr<sup>-1</sup>) available is computed from the components of the energy balance.  In GSSHA the following components are accounted for:
 
  
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''Q<sup>*</sup> - net radiation (in - out),
 
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''Q<sub>v</sub>'' - heat in precipitation,
 
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''Q<sub>e</sub>'' - heat transferred by sublimation and evaporation, and 
 
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''Q<sub>h</sub>'' - sensible heat transfer due to turbulence.
 
  
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For non-precipitation periods the net radiation is typically the dominant source of energy for melting of the snowpack (Gray and Prowse, 1993).  The net radiation is computed using Stephan-Boltzman’s law, with the assumptions that incoming radiation can be computed from the ambient temperature, ''T<sub>a</sub>''  (C), and outgoing radiation is computed assuming the snowpack is at 0&deg; C (Bras, 1990):
 
  
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| width=550 | ''Q<sup>*</sup> = 49.56 x 10-10(''T<sub>a</sub>'' + 273)4 – 27 || (92)
 
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Precipitation falling on the snowpack at temperatures above 0&deg; transmits the difference in heat between the raindrop and the snowpack.  Assuming the snowpack is at 0&deg; C and the rainfall is a ambient temperature the difference in heat energy is:
 
  
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| width=550 | ''Q<sub>v</sub>'' = ''IT<sub>a</sub>'' || (93)
 
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where:  ''I'' is the precipitation intensity (cm/hr).  Heats transferred from evaporation, sublimation, and turbulent energy are usually much smaller parts of the heat balance and are ignored in many computations (Gray and Prowse, 1993).  However, convective exchange can be significant (Linsley et al., 1982).  If the dew point is below the temperature of the snowpack, assumed to be 0&deg; C, then condensation occurs and heat is transferred (Linsley et al., 1982; Gray and Prowse, 1993).  Estimates of turbulent and latent heat exchange are usually based on measurements of air temperature, humidity, and wind speed (Gray and Prowse, 1993).  During periods of melt, the temperature of the snowpack is 0&deg; C and the saturated vapor pressure (es) is 6.11 mb (Linsley et al., 1982).  The latent heat exchange is computed assuming the latent heat of evaporation/condensation is 600 cal g<sup>-1</sup> (Anderson, 1968) and a water density of 1 g cm<sup>-3</sup> as:
 
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| width=550 | [[Image:Equation094.gif]] || (94)
 
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where:  ''r<sub>h</sub>'' is the relative humidity (%), &fnof;(V) = 0.0002 ''U'' (km/hr) (Anderson 1978), where ''U''U is the wind speed (m s<sup>-1</sup>).  Employing the Bowen ratio (Bowen, 1926) the sensible heat transfer is computed assuming the snow pack temperature is at 0&deg; C, latent heat of evaporation is 600 cal g<sup>-1</sup>, density of water is 1 g cm<sup>-3</sup>, and the Bowen ratio coefficient is 0.61 x 10-3 C<sup>-1</sup> (Bras, 1990) as:
 
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| width=550 | [[Image:Equation095.gif]] || (95)
 
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where:  ''P<sub>a</sub>'' is the atmospheric pressure (mb).
 
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For non-precipitation periods, the energy budget is calculated at an hourly time step (same as the standard hydrometeorological data), so diurnal changes in energy inputs are included in the model formulation.  During precipitation periods the energy budget is updated each overland flow routing time step (generally less than 5 minutes).
 
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The described snowfall accumulation and melting calculations proceed anytime the LONG_TERM simulation option is chosen and hourly air temperatures are provided.  If snowfall occurs, a warning will be printed to the screen and to the Summary file.  When snow accumulation occurs the amount of snow in the watershed is reported at the beginning and end of each event summary in the Summary file.
 
  
 
   '''[[Old Snow Page]]'''<br>
 
   '''[[Old Snow Page]]'''<br>

Revision as of 14:08, 28 November 2012

When GSSHA is run in the LONG_TERM simulation mode, snowfall accumulation and melting is simulated to increase its utility in regions with significant snowfall. More accurate snow accumulation and melt algorithms as well as more accurate melt transport algorithms within GSSHA are active research and model development areas at ERDC. Snowfall has a large impact on hydrologic fluxes because snowfall is normally stored for a significant period of time in the snowpack and is later released as melt water. In many parts of the world melt of the snow cover is the single most important event of the water year (Gray and Prowse, 1993). Because snowfall accumulation and subsequent melting can have such a large influence in hydrologic response of a watershed, it is important to simulate these processes. The purpose of the snowfall accumulation and melting routine is to allow an accounting of these processes with the intent to differentiate between precipitation that is rainfall that will immediately infiltrate, pond and runoff or evaporate, and snow and ice that accumulates and significantly alters the timing of hydrologic fluxes.

All three methods used within GSSHA to simulate snow accumulation and melt assume that the snow pack consists of a single layer. Certain advantages - such as time variations of liquid water content (Bloschl & Kirnbauer 1991), interflow within the snow pack layers due to ice sheets, and avalanche modeling (Colbeck 1991) - do exist when applying multi-layer snow models, but the required data to accomplish such models on a watershed level is currently unrealistic in most basins. Multi-layer snow models are typically deployed at the site-scale where spatially-close data is available.

In nature snow is a distributed process. Because of the distributed structure of the GSSHA model the snow is modeled as a distributed process. Utilizing a distributed domain gives more potential of addressing a variety of real world problems than a semi-distributed or lumped-parameter model (kirnbauer, Bloeschl et al. 1994). Because of the distributed domain, the model can also account for Orographic Effects.

GSSHA Melt Algorithms
GSSHA currently employs three snow melt models: 





 Old Snow Page


GSSHA User's Manual

9 Continuous
9.1     Computation of Evaporation and Evapo-transpiration
9.2     Computation of Soil Moisture
9.3     Hydrometeorological Data
9.4     Snowfall Accumulation and Melting
9.5     Sequence of Events During Long-Term Simulations


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