## 4 Research Results and Discussion
Panel C, in comparison to Panel B (Figure 10), presents a more consistent image of deeper parts of the Carpathian Flysch (south of the thrust), with fewer attenuated areas in the seismic record. In this result, the amplitudes observed along the Miocene reflections are more stable, whereas in Panel B, significant amplitude variations are observed. Additionally, north of the R-8 well, version C exhibits a seismic image characterized by the presence of continuous reflection sequences, which are disturbed in version B (Figures 10 and 11). In terms of accurately representing the structural variability of Miocene deposits associated with reservoir presence, reproducing the amplitude variations and geometry of reflections is crucial. In the details, attention should be mainly focused on the quality and continuity of the reflectors. For this purpose, enlarged sections of seismic profiles (Figure 10) are presented in Figure 10. Arrow symbols indicate zones where seismic imaging improvement is observed. Zone \"I\" (Figures 10 and 11) indicates a location in the northern part of the area where significant improvement in the continuity of seismic reflectors. This is likely due to the proper stabilization of the velocity field validation process in this part of the profile. These changes are marked as anomaly \"I\" in Figures 10 and 11. Other crucial areas (\"II\" and \"IIa\") present changes within the R-8 well area in the \"Raczyna-Jodlowka\" reservoir zone [27], where the distinct lining of seismic reflections defining this reservoir is observed (Figure 2). A similar situation occurs for the zone \"III\" in the \"Raczyna S\" reservoir area [27]. It corresponds to the previously described zone where an improvement in the continuity of the seismic record is observed. Considering the methodological nature of the conducted work, such a state of affairs allows for a precise interpretation of reservoir zones. The last observed zone \"IV\" is associated with the zone of reflections at the contact between flysch deposits and the crystalline basement. Using the validated VID model with SJI, a structural seismic image was reconstructed. It is worth emphasizing that a significant improvement in the seismic image has been achieved, as clearly visible in comparison to the archival results presented in Figure 2. The analysis of the above figures demonstrates the crucial role of the VID velocity field in depth processing. It can also be seen that by using the described methodology, the obtained result approaches the quality of 3D seismic processing, which provides significantly better results than 2D seismic. The results presented in the above analysis were compared to previous processing results along the Transcarpathian seismic profile (POLCRUST), confirming the correctness of the adopted data processing sequence [7; 24; 25; 26]. In order to obtain a smoother seismic image, an additional post-processing step was performed. Figure 12 shows a comparison of examples of CDP gathered from the Carpathian thrust area. Significant improvement in signal coherence can be observed on these gathers, as well as the effects of procedures such as Angle Mute, RMO update, Trim Statics, and FX filtration [40]. Figure 13 presents the result of PreSDM migration based on the seismic components shown in Figure 12, which are the result of additional processing incorporating procedures to improve signal coherence and residual RMO corrections, enhanced by the application of trim statics. This approach allows for obtaining a seismic image that is suitable for geological and reservoir interpretation at an early stage of depth imaging. Key locations on the seismic image (Figure 13) are marked with circular ellipses, confirming the correctness of the performed analyses and validating the use of independent procedures for creating VID models.