We computed annual precipitation totals for six catchments in the West and High Tatra Mountains (Roháčska, Jalovecká, Žiarska, Račkova, Tichá and Kôprová dolina) for hydrological years 1989-1998 using different interpolation and extrapolation methods. Precipitation estimates for the entire period as well as for particular hydrological years were used to compute evapotranspiration from the hydrological balance equation. The results have shown that although we used all existing precipitation data from the region along with the sophisticated methods to estimate catchment precipitation, yet, the water balance of the mountain catchments was not explained satisfactorily. and V práci sú vypočítané ročné zrážkové úhrny v šiestich povodiach Západných a Vysokých Tatier (Roháčska, Jalovecká, Žiarska, Račkova, Tichá a Kôprová dolina) pomocou rôznych interpolačných a extrapolačných metód pre hydrologické roky 1989 až1998, aj pre priemerné ročné úhrny za celé obdobie. Pre zrážkové úhrny určené rôznymi metódami bol z rovnice hydrologickej bilancie vypočítaný výpar a výsledky boli vyhodnotené opäť pre celé obdobie, aj pre jednotlové hydrologické roky. Získané výsledky ukazujú, že ani pri použití všetkých existujúcich údajov a moderných výpočtových metód existujúca meracia sieť nedáva uspokojivú odpoveď na pochybnosti, ktoré vznikajú pri určení základných prvkov hydrologickej bilancie v jednotlivých horských povodiach.
The objective of this paper is to compare the results of two distributed snow models based on different approach to snow accumulation and melt. Model WaSiM is based on the degree-day approach, while model UEB-EHZ is an energy-based model. Simulations in the mountain catchment of Jalovecký creek in winters 1989-2001 showed that both approaches can produce similar results. Model parametrization is more important than basic approach to snow accumulation and melt. Therefore, model UEB-EHZ which took into acccount influence of forest on radiation reduction and snow drift, performed better for the forest sites. The paper presents also brief overview of snow accumulation and melt modelling including calibration and verification of distributed models. Finally, it shows some outupts which can be provided by distributed snow models. and Príspevok je venovaný porovnaniu dvoch distribuovaných matematických modelov akumulácie a topenia snehu s rôznym prístupom k modelovaniu snehu. V horskom povodí Jaloveckého potoka boli hodnotené výsledky energeticky založeného modelu UEB-EHZ a modelu WaSiM, vychádzajúceho z metódy teplotného indexu pre zimy 1988/89 - 2000/2001. Porovnanie výsledkov oboch modelov ukázalo, že pokiaľ ide o základný prístup k modelovaniu topenia snehu (energetická bilancia alebo teplotný index), nemohli sme v danom povodí určiť, ktorý z nich viedol k lepším výsledkom. Väčší vplyv na simuláciu vodnej hodnoty snehu ako výber základného prístupu k modelovaniu akumulácie a topenia snehu, má parametrizácia konkrétneho modelu. V modeli UEB-EHZ bol napríklad čiastočne zahrnutý vplyv lesa na globálne žiarenie a podmienky ukladania snehu (drift). Preto bolo topenie snehovej pokrývky v lese týmto modelom simulované reálnejšie ako modelom WaSiM. Okrem porovnania výsledkov dvoch základných prístupov k modelovaniu akumulácie a topenia snehu v horskom povodí príspevok ukazuje aj niektoré výstupy, ktoré možno získať pomocou distribuovaného snehového modelu a stručne sa zaoberá diskusiou o kalibrácii a validácii takéhoto modelu.
This study evaluates MODIS snow cover characteristics for large number of snowmelt runoff events in 145 catchments from 9 countries in Europe. The analysis is based on open discharge daily time series from the Global Runoff Data Center database and daily MODIS snow cover data. Runoff events are identified by a base flow separation approach. The MODIS snow cover characteristics are derived from Terra 500 m observations (MOD10A1 dataset, V005) in the period 2000–2015 and include snow cover area, cloud coverage, regional snowline elevation (RSLE) and its changes during the snowmelt runoff events. The snowmelt events are identified by using estimated RSLE changes during a runoff event. The results indicate that in the majority of catchments there are between 3 and 6 snowmelt runoff events per year. The mean duration between the start and peak of snowmelt runoff events is about 3 days and the proportion of snowmelt events in all runoff events tends to increase with the maximum elevation of catchments. Clouds limit the estimation of snow cover area and RSLE, particularly for dates of runoff peaks. In most of the catchments, the median of cloud coverage during runoff peaks is larger than 80%. The mean minimum RSLE, which represents the conditions at the beginning of snowmelt events, is situated approximately at the mean catchment elevation. It means that snowmelt events do not start only during maximum snow cover conditions, but also after this maximum. The mean RSLE during snowmelt peaks is on average 170 m lower than at the start of the snowmelt events, but there is a large regional variability.
Spatial and temporal variability of snow line (SL) elevation, snow cover area (SCA) and depletion (SCD) in winters 2001-2014 is investigated in ten main Slovak river basins (the Western Carpathians). Daily satellite snow cover maps from MODIS Terra (MOD10A1, V005) and Aqua (MYD10A1, V005) with resolution 500 m are used. The results indicate three groups of basins with similar variability in the SL elevation. The first includes basins with maximum elevations above 1500 m a.s.l. (Poprad, Upper Váh, Hron, Hornád). Winter median SL is equal or close to minimum basin elevation in snow rich winters in these basins. Even in snow poor winters is SL close to the basin mean. Second group consists of mid-altitude basins with maximum elevation around 1000 m a.s.l. (Slaná, Ipeľ, Nitra, Bodrog). Median SL varies between 150 and 550 m a.s.l. in January and February, which represents approximately 40–80% snow coverage. Median SL is near the maximum basin elevation during the snow poor winters. This means that basins are in such winters snow free approximately 50% of days in January and February. The third group includes the Rudava/Myjava and Lower Váh/Danube. These basins have their maximum altitude less than 700 m a.s.l. and only a small part of these basins is covered with snow even during the snow rich winters. The evaluation of SCA shows that snow cover typically starts in December and last to February. In the highest basins (Poprad, Upper Váh), the snow season sometimes tends to start earlier (November) and lasts to March/April. The median of SCA is, however, less than 10% in these months. The median SCA of entire winter season is above 70% in the highest basins (Poprad, Upper Váh, Hron), ranges between 30-60% in the mid-altitude basins (Hornád, Slaná, Ipeľ, Nitra, Bodrog) and is less than 1% in the Myjava/Rudava and Lower Váh/Danube basins. However, there is a considerable variability in seasonal coverage between the years. Our results indicate that there is no significant trend in mean SCA in the period 2001-2014, but periods with larger and smaller SCA exist. Winters in the period 2002-2006 have noticeably larger mean SCA than those in the period 2007-2012. Snow depletion curves (SDC) do not have a simple evolution in most winters. The snowmelt tends to start between early February and the end of March. The snowmelt lasts between 8 and 15 days on average in lowland and high mountain basins, respectively. Interestingly, the variability in SDC between the winters is much larger than between the basins.