Unraveling the Origin of the Messinian? Evaporites in Zakynthos Island, Ionian Sea: Implications for the Sealing Capacity in the Mediterranean Sea

Abstract

The new approach on depositional conditions of the Messinian evaporites in Zakynthos Island indicates that the evaporites in the Kalamaki and Ag. Sostis areas were redeposited during the Early Pliocene. They accumulated either as turbiditic evaporites or as slumped blocks, as a response to Kalamaki thrust activity. Thrust activity developed a narrow and restricted Kalamaki foreland basin with the uplifted orogenic wedge consisting of Messinian evaporites. These evaporites eroded and redeposited in the foreland basin as submarine fans with turbiditic currents or slumped blocks (olistholiths) that consist of Messinian evaporites. These conditions occurred just before the inundation of the Mediterranean, during or prior to the Early Pliocene (Zanclean). Following the re-sedimentation of the Messinian evaporites, the inundation of the Mediterranean produced the “Lago Mare” fine-grained sediments that rest unconformably over the resedimented evaporites. The “Trubi” limestones were deposited later. It is critical to understand the origin of the “Messinian” Evaporites because they can serve as an effective seal rock for the oil and gas industry. It is thus important to evaluate their thickness and distribution into the SE Mediterranean Sea.

Contrasting Styles of Salt‐Tectonic Processes in the Ionian Zone (Greece and Albania): Integrating Surface Geology, Subsurface Data, and Experimental Models

“…(2018), Lacombe et al. (2009), Papanikolaou (2021), and Schröder (1986)) and Pliocene to Holocene in the outermost (western and offshore) thrusts (e.g., Aliaj & Mesonjesi, 2022; Clews, 1989; Kamberis et al., 1996; Karakitsios et al., 2017; Kokkalas et al., 2013; Mercier et al., 1972; Nieuwland et al., 2001; Sorel et al., 1976; Speranza et al., 1995; Underhill, 1988, 1989; van Hinsbergen et al., 2006; Zelilidis et al., 2023).…”

“…The age succession describes a piggyback thrust system, with ages varying progressively from late Eocene to early Oligocene for the thrusting of the Pindos Flysch in the east and Aquitanian-Burdigalian in its innermost (eastern) part (Avramidis et al, 2000;Botziolis et al, 2021;Clews, 1989;IFP, 1966;Jenkins, 1972;Kamberis et al, 2000;Makrodimitras et al, 2010;Nieuwland et al, 2001;Pieri, 1990;Roure et al, 2004;Savoyat, 1977;Sejdini et al, 1994;Sotiropoulos et al, 2003;Speranza et al, 1992;Van Geet et al, 2002) to post-Messinian (affecting evaporites of this age; see Aliaj (2006), Kokkalas et al (2013), Kosmidou et al (2018), Lacombe et al (2009), Papanikolaou (2021), andSchröder (1986)) and Pliocene to Holocene in the outermost (western and offshore) thrusts (e.g., Aliaj & Mesonjesi, 2022;Clews, 1989;Kamberis et al, 1996;Karakitsios et al, 2017;Kokkalas et al, 2013;Mercier et al, 1972;Nieuwland et al, 2001;Sorel et al, 1976;Speranza et al, 1995;Underhill, 1988Underhill, , 1989van Hinsbergen et al, 2006;Zelilidis et al, 2023).…”