## 5 Discussion
Sedimentary rocks (Neogene and Paleogene) are relatively homogeneous in density and non-magnetic, and therefore their role in density anomalies is less evident. The volcanic rocks extend into the area of interest from the north, which is reflected in the CBA map by a group of smaller, relatively fragmented anomalies. Their intensity is directly proportional to the represented amount of solid volcanic bodies in the volcanic complex as well as the thickness of this complex. Pyrocastic breccias and deposits of pyroclastic lava flows, as well as effusive cones [42], cause a positive anomaly. A positive anomaly in the vicinity of Vinne (castle) is composed of pyroxenic-amphibolite andesites, which form mostly extrusive domes that often pass into thick lava flows [24]. Extrusive bodies of andesites outcropping in the SW part of the neovolcanics are also significantly reflected in the gravity field. According to the field map of the CBA, it can be assumed that volcanic rocks are also located in the area of Zemplinska Sirava where borehole GTH-1 was drilled. During this research, volcano-sedimentary sequences were compared [43; 44; 45] to geoelectric and gravimetric profiles. In the case of profile PF 5, there was no visible difference between them. The differences in the different basement depths are no more than 50 m. As already mentioned, the problem in the interpretation of geoelectrics is that the resistance intervals of the individual layers are overlapping. For this reason, only one geoelectric  
Figure 9: The Humenné Unit has an elongated shape with an irregular depth of the main aquifer. Based on geophysical methods, the system of tectonic elevations and grabens was identified. (**A**) Uncovered geological map respects the main tectonic deformations and geological structure of the Humenné Unit. (**B**) Borehole GTH-1 at a depth of 500 m confirms yield ranging from 3.5 to 4.2 \(\mathrm{\SIUnitSymbol{s}^{-1}}\) and a temperature of 42 \(\mathrm{\SIUnitSymbol{s}^{-1}}\). (**C**) Isotherm’s model on the pre-Cenozoic surface displays increasing temperatures toward the center of the Eastern Slovak Basin and confirms relationships between elevations and temperature distribution. (**D**) Geological cross-section along the Hummene unit confirms tectonic erosional processes during Cenozoic evolution. horizon was allocated to representing a Cenozoic fill (4-50 \(\Omega\)m). With increasing depths, the resistance increases less significantly, which may correspond to non-carbonate Mesozoic rocks. But, in other cases, where volcanic rocks contain groundwater, the volume of electrical resistivity rate is 350-500 \(\Omega\)m.  
The assessment of the geothermal activity of the area is best interpreted based on the earth's heat flow data. Data from wells available in the evaluated area showed a heat flow density in the range of 73.3 to 94.8 mW/m\({}^{2}\). The input parameters for the calculation of the perspective specific heat-energy potential represent values of porosity, rock bulk density, specific heat of rocks, specific density and heat of geothermal water (Figure 9C), reservoir temperature on the collector's surface, neutral zone temperature, collector thickness of geothermal water, and the reduction coefficient. Based on the mentioned data, the values of the perspective specific heat-energy potential of geothermal energy reserves for the Triassic carbonate formation were calculated. The results of the calculations were values with a wide range of 0.337-19.533 GJ/m\({}^{2}\). The wide range is related to the unit's occurrence on the surface in the central area up to a depth of \(-2250\) m. The thickness of the collectors does not significantly affect the changes in the values of the specific thermal energy potential, as it is around 1000 m throughout the whole structure and shows only a small variability (850-1120 m) [22].