Fig 2 - uploaded by Gregor Kovačič
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Simplified geological map of the Velika planina plateau with proved and supposed groundwater connections (after Premru 1982, Novak 1994/95).
Source publication
The present paper presents the hazard mapping of groundwater on the Velika planina alpine karst plateau. There are no permanent residents on the plateau. Nevertheless, some serious hazards to the quality of the respective karst springs are arising from sports, tourist and farming activities. Some pollution has been already recorded in springs, show...
Contexts in source publication
Context 1
... with the associated pastures. These are Velika, Mala and Gojška planina (planina = mountain meadow), which extend from Šimnovec on the west to Marjanine njive on the east. Meadows stretch from Kisovec in the south and pass over to the forest ranges and further towards planina Konjščica and Dol to the north. The studied area covers 36.5 km 2 (Fig. ...
Context 2
... are no surface running waters present on the plateau, only a few smaller springs appear which are commonly captured and used for the individual water supply of nearby mountain lodges and holiday huts. In the margins of the Velika planina plateau several springs occur, some of these also are captured for the water supply of small areas. In Fig. 2 only the important springs are ...
Context 3
... of the groundwater flow have shown that the autochthonous precipitation water from the surface of the Velika planina plateau percolates directly into the karst aquifer and runs mostly towards the Lučnica karst spring (Fig. 2). Important outflows are also in the area of Dolski potok, Konjski potok, springs Krivčevo, Šunce, Brložnica and some smaller springs in the Črna valley (Novak & Bizjak 1989, Novak ...
Citations
The Late Oligocene pre-Eonile paleoriver flows northwesterly over the Eocene Limestone Plateau in the east central Western Desert, west of the Nile Valley (Sohag), building an alluvial plain and leading to the karstification of the limestone bedrock, as paleoerosional surfaces and paleodolines. Knowledge of this alluvial karstification is completed with the detailed studies of the sedimentary evolution of the fluvial system and its contemporary deposition. Analysis of the sedimentological and geomorphological features allows discussing the natural environmental conditions that favored karst in the past and its main genetic mechanisms. The architectural elements of the fluvial deposits indicate that they were deposited in a gravel-dominated braided fluvial system, characterized by high availability of water and sediment supplies. The current study proves that genesis of paleodolines was mainly related to this high water supply. Some of them were progressively filled by syn-sedimentary deformed unconsolidated deposits. Such deformation is due to dissolution of the underlying sagging synclinal limestone, conditioning the location of sinking waters where preferential dissolution and later suffosion took place. A model for the evolution of the paleodoline fills is proposed and interpreted in three different stages: (1) gravitational processes developed and disorganized gravels were remobilized and dragged toward the created paleodolines; (2) flooding of the paleodolines acted as lakes where Gilbert-type deltas and gravel slope deposits accumulated, exhibiting several unconformities interpreted as a result of continued subsidence of the paleodoline related to dissolution; and (3) nondeformed fluvial facies sealed the whole deposits, marking the end of the karstification process. Combinations of different types of factors that could cause karstic subsidence and associated hazards include soluble rock lithology, paleoclimate, and deformational structure.
