## 3 Materials and Methods
### Basin Modeling  
The geological, geophysical, and reservoir mechanical parameters have been incorporated into the 2D basin models during the model building phase [64] that was carried out with the Schlumberger PetroMod software (version 2017.1). Moreover, recently published calibration models have been added to the Calibration Editor. The main purpose of the 2D basin modeling studies focus on the better understanding of the hydrocarbon systems or providing a more adequate regional overview [65; 66; 67]. This study delivers an alternative usage in case of 2D basin models; the original concept was to extend the application of basin modeling in the field of engineering sciences. Depth-converted seismic horizons delivered the timeframe and the sedimentation rate to the simulated geological sections that starts from the deposition of the Middle Miocene. The seismic horizons have been correlated from magnetostratigraphic absolute age well picks [68; 69; 70; 71; 72; 73]. The continuous sedimentation has been interrupted three times by discordance surfaces. The amount of eroded strata thicknesses is variable along the sections, but both have been integrated into the numerical simulations. The layers between the depth horizons consist of more lithofacies, because the sedimentation has been controlled by a programing delta series from the Late Miocene (Figure 8). Twelve layers have been separated during the model building phase; the layers consist of 5 to 20 sublayers due to the lithological heterogeneities within the prograding delta series (195 sublayers). The direction of Section_01 is parallel with the sediment transport direction and 168 km long, but the Section_01A is perpendicular to the sediment influx with 189 km total length. The delineation of lithofacies is relied on the evaluation of the lithology-sensitive well logs and the identified clinoforms [28]. One lithofacies has been attached to every Late Miocene and younger formations; only the prodelta turbidites (Szolnok Fm.) have been divided into two parts (shaly siltone and silty sandstone) with the calculated shale volumes. A unique porosity-effective stress trend has been assigned to every lithofacies, and a poropperm trend has been fitted to the compaction trends that are consistent with the measured permeability data (Hg saturated, Nano-K). Two boundary conditions have been estimated for every time step as thermal boundary conditions, the sediment water interface temperature (SWIT) and the basal heat flow. The SWIT represents the upper thermal boundary or the initial sediment temperature when the burial started. The SWIT has been calculated with the built-in model from paleo water depth values [74] that originated from laboratory reports and published data [75]. The paleo heat flow has been reconstructed with the McKenzie [76] crustal heat flow model that is able to estimate the stretching factors from the current and the paleo burial curves along the simulated section. The stretching factors change along the simulated sections, the magnitude of the crustal stretching factor falls into the 1.4-2 interval, but the stretching of the lithospheric mantle has a higher variance (3 to 5). The applied factor values are coherent with the non-uniform stretching concept that was suggested by previous studies in case of the Pannonian Basin [77,78]. The basal heat flow has been calculated from the stretching factors along the models and published thermal parameters have been considered [21,79]. The simulation of the basin models is a multi-phase iterative process that aims to reduce the difference between the simulated and the measured parameters. At least four recommended parameters must be involved in the calibration (pore pressure, porosity, temperature, and maturity) [48]. The calibration has a logical order that starts with the pore pressure, because it determines the effective stress, which controls the porosity.