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The present paper continues with the research in the HPFZ. To study the relationship between groundwater level changes and seismic events is the key point of this study.
Two seismic stations, Ostas (OSTC) and Chvalec (CHVC), are operated by the Institute of Rock Structure and Mechanics, Academy of Sciences of the Czech Republic (ASCR), in the area of the HPFZ. In addition, two other stations, Dobruska-Polom (DPC) and Upice (UPC), operated by the Institute of Geophysics, ASCR are located nearby (e.g.
All three wells are located in the distance of 8 to 10 km from the HPFZ. The HJ-2 well lies south of the fault and VS-3 and V-34 wells are north of it, see Figure 1.
Although the events in Figure 5 are selected so that they are located at the HPFZ or in the close vicinity of the wells, we do not find any remarkable drops or rises of the water levels in the given time period.
As it has been assumed, the earthquakes are located mainly close to the HPFZ, see Figure 3.
We derived the Smf index for the SW marginal scarp of the Jestrebi Mts which we suppose to be fixed to the anticipated normal fault parallel to the main reverse fault of the HPFZ (see also Stejskal et al., 2006).
In total five profiles, crossing both the anticipated faults and the main reverse fault of the HPFZ, were measured at three sites on both sides of the NW part of the HPT (see Fig.
Based on the results of resistivity measurements we suppose that the NE margin of the studied part of the HPT is controlled by a normal fault parallel to the main reverse fault of the HPFZ. The position of this fault is corresponding to the foothill of the Jestrebi Mts.
The HPFZ belongs to the broader seismoactive area of the NE margin of the Bohemian Massif which spreads between the Krkonose Mts.
The Hronov-Porici Fault Zone (HPFZ) is a system of parallel fractures, dividing two important structural units--Intrasudetic Depression and the Krkonose Piedmont Basin (Fig.
The relatively frequent local seismic activity is a proof of the current mobility of the HPFZ. Macroseismic effects of historical earthquakes in this area reached the epicentral intensity [I.sub.o] = 7[degrees] three times during the last 300 years (30 June 1751, 11 December 1799 and 10 January 1901--Karnik et al., 1958).
A major role in the transport of the mantle derived C[O.sub.2] play deep permeable faults like the HPFZ or some other local fractures (Jetel and Rybarova, 1979).
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