Geology Without Limits and Soyuzmorgeo in the Black Sea Scientific Exploration
Program (Graham et al. 2013; Nikishin et al. 2015a, b).
In this perspective it was highlighted that reprocessing the vintage OGS seismic
data using up-to-date methods could increase the image quality and interpretability
of the existing data sets (Fig. 6.2). Funding for reprocessing was provided also by
CGG GeoSpec. The reprocessed data set have been then integrated with the existing
published sections and wells resulting in a regional geological interpretation across
the Western Black Sea Basin with the prolongation of geological data from the
well-studied North Western Romanian-Bulgarian shelf to less constrained deep
water basin and Turkish shelf area.
6.1.1 Inferences Over the Black Sea Basin Evolution
The roll-back associated with the N-ward subduction of Neotethys under the
Rhodope–Pontides Arc opened the Western Black Sea back-arc basin during
(Adamia et al. 1977; Dinu et al. 2005; G€ orür 1988; Letouzey et al. 1977;
Zonenshain and Le Pichon 1986) latest Cretaceous–Middle Eocene times
(Fig. 6.3, Munteanu et al. 2011; Robinson et al. 1995). This extensional stage
resulted in the formation of two oceanic crust overlain by an up to 15 km thick
sedimentary sequence in their centre (Neprochnov et al. 1970; Shillington et al.
2008; Graham et al. 2013; Nikishin et al. 2015a). Shortly after this extensional
period, as a result of the Pontides/Taurides continental collision, inversion of both
sub-basins started with the Late Middle Eocene times (Dinu et al. 2005; Finetti et al.
1988; Hippolyte et al. 2015; Khriachtchevskaia et al. 2010; Okay et al. 1994;
Sinclair et al. 1997; Yilmaz et al. 1997). The far-field transmission of contractional
deformation from the Balkan-Pontides Indentor to the Romanian-Ukrainian Offshore resulted in the inversion of pre-existing extensional structures and the formation of a North-vergent thick-skinned thrust system in the Western Black Sea
(Figs. 6.1 and 6.3, Munteanu et al. 2011). The Late Eocene-Pliocene compressional
structures changes polarity along the basin strike, from north-vergent in the west to
south-vergent in the east, as inferred by observations and analogue modelling
studies (e.g., Munteanu et al. 2011, 2013). Hence the S-ward indentation of Crimea
and Caucasus created an S-vergent thick-skinned thrust system in the Eastern Black
Sea (Finetti et al. 1988; Nikishin et al. 2015a, b). A large transfer zone including the
Odessa–West Crimea fault and Mid–Black Sea High accommodates the overall
contractional polarity change during Late Eocene–Pliocene times (Finetti et al.
1988; Starostenko et al. 2015). The measured total amount of shortening recorded
across the entire Black Sea domain is in the order of 30–40 km (e.g., Munteanu
et al. 2011 and reference therein).
6 New Insights into the Black Sea Basin, in the Light of the Reprocessing of. . .
93
Program (Graham et al. 2013; Nikishin et al. 2015a, b).
In this perspective it was highlighted that reprocessing the vintage OGS seismic
data using up-to-date methods could increase the image quality and interpretability
of the existing data sets (Fig. 6.2). Funding for reprocessing was provided also by
CGG GeoSpec. The reprocessed data set have been then integrated with the existing
published sections and wells resulting in a regional geological interpretation across
the Western Black Sea Basin with the prolongation of geological data from the
well-studied North Western Romanian-Bulgarian shelf to less constrained deep
water basin and Turkish shelf area.
6.1.1 Inferences Over the Black Sea Basin Evolution
The roll-back associated with the N-ward subduction of Neotethys under the
Rhodope–Pontides Arc opened the Western Black Sea back-arc basin during
(Adamia et al. 1977; Dinu et al. 2005; G€ orür 1988; Letouzey et al. 1977;
Zonenshain and Le Pichon 1986) latest Cretaceous–Middle Eocene times
(Fig. 6.3, Munteanu et al. 2011; Robinson et al. 1995). This extensional stage
resulted in the formation of two oceanic crust overlain by an up to 15 km thick
sedimentary sequence in their centre (Neprochnov et al. 1970; Shillington et al.
2008; Graham et al. 2013; Nikishin et al. 2015a). Shortly after this extensional
period, as a result of the Pontides/Taurides continental collision, inversion of both
sub-basins started with the Late Middle Eocene times (Dinu et al. 2005; Finetti et al.
1988; Hippolyte et al. 2015; Khriachtchevskaia et al. 2010; Okay et al. 1994;
Sinclair et al. 1997; Yilmaz et al. 1997). The far-field transmission of contractional
deformation from the Balkan-Pontides Indentor to the Romanian-Ukrainian Offshore resulted in the inversion of pre-existing extensional structures and the formation of a North-vergent thick-skinned thrust system in the Western Black Sea
(Figs. 6.1 and 6.3, Munteanu et al. 2011). The Late Eocene-Pliocene compressional
structures changes polarity along the basin strike, from north-vergent in the west to
south-vergent in the east, as inferred by observations and analogue modelling
studies (e.g., Munteanu et al. 2011, 2013). Hence the S-ward indentation of Crimea
and Caucasus created an S-vergent thick-skinned thrust system in the Eastern Black
Sea (Finetti et al. 1988; Nikishin et al. 2015a, b). A large transfer zone including the
Odessa–West Crimea fault and Mid–Black Sea High accommodates the overall
contractional polarity change during Late Eocene–Pliocene times (Finetti et al.
1988; Starostenko et al. 2015). The measured total amount of shortening recorded
across the entire Black Sea domain is in the order of 30–40 km (e.g., Munteanu
et al. 2011 and reference therein).
6 New Insights into the Black Sea Basin, in the Light of the Reprocessing of. . .
93