Figure 2- - uploaded by Evangelos Kamperis
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Geological map of the Klokova-Varassova area. Location A in figure 1a (Sotiropoulos, 2005). A narrow elongated area occupied by hills (i.e. Mavrovouni hill), is located between Varassova and Klokova mountains). It represents a pop-up structure bounding to the west and to the east by thrust faults (figures 2 & 3, Sotiropoulos et al., 2003). Heading eastwards, close to the western flank of Klokova mountain, another thrust fault was identified. It is a NNW-SSE trending and east-dipping thrust fault that runs parallel to the axis of Klokova anticline. Its northern prolongation reaches up to the Evinos river (Sotiropoulos 2005, figure 2).
Contexts in source publication
Context 1
... authors consider that GT represents an inverse fault (Aubouin, 1959;IFP, 1966;BP, 1971), while others support that is a major thrust, accompanied with great displacement (Fleury, 1980, Kamberis et al. 2000, Sotiropoulos et al., 2003. In this position, Cretaceous limestones thrust over flysch sediments of Ionian zone ( figure 2). A west-verging narrow asymmetric anticline plunging to the north lies on the hangingwall of the GT. ...
Context 2
... short forelimb is characterized by subvertical strata while the backlimb by east to northeast dipping strata (figure 2). The flysch on the footwall block is intensively deformed by imbricates and tight folding in particular at the northwestern slopes of Varassova mountain ( Sotiropoulos et al., 2003, figure 2). ...
Context 3
... is mapped on the north-western slopes of Skolis mountain induced the repetition of the carbonate series (figure 5). The above faults are considered to be splays rooting on the main thrust fault (Kamberis et al, 2000). Concerning the age of the GT emplacement in the study area, a late Oligocene age is inferred by the age determinations of the younger flysch members that outcrop west of Skolis mountain ( Kamberis et al., 2000Kamberis et al., , 2005). ...
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Citations
The spatial-temporal evolution of seismicity is examined, during the initial impoundment of Pournari reservoir located on Arachthos River (Western Greece), as well as for the next 30 years. The results show that, despite the relatively moderate-to-high seismicity from west to east, there is no remarkable earthquake in the vicinity before the first reservoir impoundment. Immediately after the impoundment (January 1981), and during the first 4 months, a considerable number of low-magnitude seismic events were recorded in the broader area of the dam. Moreover, two independent major events occurred on March 10, 1981 (M
L
= 5.6) and April 10, 1981 (M
L
= 4.7) with focal depths 13 and 10 km, respectively. The detailed analysis of the two corresponding aftershock sequences shows that they present different behaviors (e.g., larger b-value and lower magnitude of the main aftershock) than that of other aftershock sequences in Greece. This seismicity is probably due to triggering, via the water loading mechanism and the undrained response due to a flysch appearance on the reservoir basement. The activation of the thrust fault may be attributed to the bulging of evaporites that characterize the disordered structure of W. Greece, via possible water intake. The detailed processing of the recorded seismicity during the period 1982–2010, in comparison with the variations of Pournari Dam water level, shows an increase of shallow seismicity (h ≤ 5 km) in the vicinity of the reservoir up to a 10-km distance—in contrast to the initial period, characterized by a number of deeper events due to the background response change from undrained to drained status.
