Facskó Ferenc (szerk.) (2012): Kutatások a Nyugat-magyarországi

Kutatások a Nyugat-magyarországi Egyetemen
roundings surfaces into the karren forms on bare slopes. Therefore the solution capacity
does not decrease along the slope downwards but increases. The solution capacity is small
but scattered on the upper part of the bare slope. The solution is intensive and concentrated
on the upper part of the slope with plant patch. The increasing of the karren features are different
on the bare slopes and slopes with a plant patch. Karren features rather widen on bare
slopes, while they rather deepen on slopes with a plant patch. The specifi c width is greater
on slope with Pinus mugo than on slopes with grass patch, and the specifi c cross-section area
of the channel is also greater. Hence the solution intensivity is greater on slopes with Pinus
mugo than on slopes with a grass patch.
VERESS M. – ZENTAI Z. – PÉNTEK K. – MITRE Z. (2011): Rinnenkarr rendszerek fejlődése.
Karsztfejlődés XVI. NYME Kiadó, TTK Természetröldrajzi Tanszék gondozásában p.
71-85.
Abstract – We measured the depth and the width of the main channels of three channel systems,
the distance between the measuring points was 10 centimetres. These channels occur
on the fl oor of the glacier valley, which is under the Tragl peak in the Totes Gebirge. By using
these data we calculated the cross-section areas of the channel (as the product of the width
and the depth of the channel) along the profi le. We found that main channel of the channel
system marked V/1 has the most regular data among the investigated channels. Connection
was examined between the distance measured from the margin of the slope (x[m]) and the
cross-section area (T[cm2]) here. We found that cross-section area data heaps have their
own local maxima. These places are located on the main channels at 1-2 decimeter distance
towards the dip direction of the slope from the connecting sites of the tributary channels.
Further on, it may also be seen that there is direct proportion between the length of the
tributary channels and the maximum cross-section area. The longer the tributary channel,
the greater the increase of the main channel cross-section area. Probably, the cause of
the phenomena is that the water fl owing from the tributary channel into the main channel
contributes to the solution. Although the water of the tributary channel may be saturated,
turbulence probably causes dissolution as a result of mixing of the water of the tributary
channel and the main channel. As for the turbulence the main channels can be classifi ed as
continuously turbulent and non-continuously turbulent channels. In the non-continuously
turbulent main channels there are separated turbulent zones in the rivulets of the main
channel as tributary channels can be found rarely. In case of continuously turbulent main
channels, the water fl ow of the main channel is unique as the tributary channels have great
density along the main channel. In case of only few type B tributary channels, the turbulent
fl ow will be weak or it does not develop at all.
VERESS M. (2012): Fedőüledékes depressziók típusai és kialakulásuk. Földrajzi Közlemények,
136. 1. p. 2-21.
Abstract – In this study we present closed features of the superfi cial deposit of the karst.
Our researches areas were the following: karst areas of Hungary, a few karst areas of the
Alps and the Padis Plateau (Apuseni Mountains, Romania). We investigated the morphology
of the depressions of superfi cial deposit (topographical mapping, morphological mapping)
further more the morphology of the bedrock (Vertical Electrical Sounding). We
analysed the denudation types of superfi cial deposit found at the bottom of depressions of
bedrock (topographical map, and the usage of slope angle class data). In this study depressions
of superfi cial deposit were classifi ed. These are the following: karst margin and karst
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