Assessments of the infiltration recharge of groundwater are performed using various methods and on different scales. Infiltration is dependent of climatic factors, aspects of water circulation, as well as on quasi-stationary and variable environmental features of a specific area, which are frequently difficult to determine on the basis of direct measurements or observations.
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Our analysis has indicated favourable and unfavourable conditions for recharge of groundwater in the annual period and in both half-year periods, which are the result of mutual relationships between the physical qualities of these catchment areas and their climatic and hydrological characteristics.
The results obtained also confirmed the impact of surface runoff and actual evapotranspiration on the spatial distribution of effective infiltration. With soil types and groundwater depth distributions being similar in the catchment areas, changes in relationships between components of water balance are caused by differences in the type of land usage.
Application of the WetSpass model has made it possible to arrive at a more accurate assessment of groundwater recharge. The results obtained may be used for erification of recharge areas and values of effective infiltration, set as a boundary condition in groundwater flow models. Band L. Cadenasso M.
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Heterogeneity in Urban Ecosystems: Pattern and Process. Jones C. Eds : Ecosystem Function in Heterogeneous Landscapes. Springer-Verlag New York — pp. Batelaan O. WetSpass: a flexible GIS based distributed recharge methodology for regional groundwater modelling. Peters J. Hoehn E.
Jensen K. Leibundgut C. Griffioen J. Webb B. IAHS Publ. Characterizing groundwater recharge and discharge using remote sensing GIS ecology hydrochemistry and groundwater modeling. Arcview interface for WetSpass. Version Scaling in hydrology. Hydrological Processes 15 — Brun S.
Groundwater: Resource Evaluation, Augmentation, Contamination, Restoration, Modeling and Management
Simulating runoff behavior in an urbanizing watershed. Computers Environment and Urban Systems 24 5— Callahan T. Vulava V. Passarello M. Estimating groundwater recharge in lowland watersheds.
Hydrological Processes 26 — Cherkauer D. A Estimating ground water recharge from topography hydrogeology and land cover Ground Water 43 — Chiang W. Springer-Verlag Berlin pp.
Recharging infiltration of precipitation water through the light soil in the absence of surface runoff. Journal of Water and Land Development 32 25— Eds : Wody powierzchniowe Poznania. Water problems in urban areas ]. Nowicki K. Metodyka modelowania matematycznego w badaniach i obliczeniach hydrogeologicznych. Poradnik metodyczny [ Methodology of mathematical modeling in hydrogeological research and calculations. Methodical guide ].
Bogucki Wyd. De Vries J. Groundwater recharge: an overview of processes and challenges. Hydrogeology Journal 10 5— Dripps W. A simple daily soil-water balance model for estimating the spatial and temporal distribution of groundwater recharge in temperate humid areas. Hydrogeology Journal 15 — Duda R. Farat R.
Graf R. Nauka Przyroda Technologie 7 1— Estimation of shallow groundwater recharge using a GIS-based distributed water balance model. Quaestiones Geographicae 33 27— Green W. Studies on soil physics The flow of air and water through soils. Journal Agriulture Science 4 1— Gurwin J. Acta Universitatis Wratislaviensis pp. Healy R. Lithological unit B includes fluvio-lacustrine formations digitization, their density was calculated in ArcMap Despite the fact that marbles of the area have Density command.
Next, a reclassification of the raster linea- high infiltration coefficient, a rating of 60 was given owing to their ment-density file followed, into 5 classes, from very low to very local interest of groundwater lithological unit C. This lithological high, according to the class boundaries of Table 3, yielding Fig. The lineament density raster file was assigned a weight of talus cones.
It can be noticed that in the mations. The formation lithological unit E with the highest rating area of red color, where no faults and lineaments exist, the poten- is alluvial deposits due to the high infiltration coefficient and tiality of the presence of groundwater is low, in contrast with the the high storativity capacity of groundwater.
Distribution of the groundwater potentiality first pair of numbers in legend based on slope left and drainage network density right , divided into classes. Slope recharge rate and vice versa. In general, water potentiality final map, according to AHP methodology. Usually, the steep 4. Depth to groundwater slopes indicate greater water velocity. Therefore, it is observed that in the areas of steeper relief the runoff is increased.
This in turn The depth to groundwater is defined as the distance from the minimizes the degree of groundwater recharge Doll et al. The water table is highest in April— groundwater potentiality increases due to greater infiltration, that May and lowest in early October depending on meteorological con- is the lower the slope, the greater the recharge Fig. The slope ditions. Water level mea- methodology.
The depth to groundwater in the alluvial aquifer ranges from less than 3 to 4.
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Drainage density more than 25 m below ground surface, while the depth in the mar- bles aquifer ranges between 15 and m. The resulting map was Drainage density is the total length of all the streams and rivers classified into five major classes Table 3 and Fig. In the green-colored by stream channels.