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28
63 rd EASTERN SNOW CONFERENCE
Newark, Delaware USA 2006
the observed pattern. Inadequacies arise from processes not included in the model such as
redistribution of snow by wind and avalanches (Blöschl et al., 1991; Lehning et al., 2000;
Doorschot et al., 2001). At such small scale and with the adoption of such a high spatial resolution
we can see the role of snow redistribution and understand how distributed models have to be
improved to account for such processes.
Runoff simulations
For the 2005 melt season (calibration period) discharge data have been available for the period
of 9 July–30 September (Figure 5).
Figure 5. Simulated icemelt averaged over the catchment area, M (mm h –1 ), hourly data of air temperature, T
(°C), and precipitation P (mm h –1 ) at Hoher Sonnblick observatory, and observed and simulated discharge Q
(m³ s –1 ) at the catchment outlet of Goldbergkees. The increasing lines at the bottom plot indicate the
cumulated discharge Q cum (10 6 m³) over the period of the discharge observations from 10 July to 30
September 2005.
The beginning of the observations shows rain-induced discharge peaks. Typical diurnal
variations of the observed runoff, induced by icemelt are seen in the period from end of August
until mid of September. The performance of the simulation has been employed according to the
efficiency criterion R NS² (Nash and Sutcliffe, 1970), defined as: