## 2 Geological Setting, Lithology and Bio-Magnetostrigraphic Framework  
The Baskil section outcrops in eastern Turkey, at ca. 19.8 km NW of the town of Baskil (38 deg36'30.34'' \(\mathrm{N}\), 38 deg36'03.46'' \(\mathrm{E}\)) (Figure 1). This section is part of the Kirkgecit Formation in the Elazig Basin and was deposited at a paleo-water depth of \(\sim\)300-600 m [33]. The total thickness of the section is 385 m and covers the upper part of the Lutetian up to the lowermost part of the Bartonian [33]. The present study considers the interval from 120 to 200 m that encompasses the MECO event [3; 33]. This interval consists of massive hemipelagic marlstone beds, containing calcareous plankton and benthic foraminifera, intercalated with calcarenite beds 15 cm to 1 m thick, representing a mixture of siliciclastic grains and bioclasts and including several large benthic foraminifera (LBF) [41; 42]. Seven of these turbidites are recorded in the analyzed interval and allowed to define the Shallow Benthic Zones (Figure 2). The hemipelagic sedimentary rocks are interpreted to have been deposited in a back-arc basin on continental crust [43]. Within the Kirkgecit Formation, the Baskil section has not been deformed and does not show alteration despite the regionally active tectonic regime. High-resolution integrated magneto- and biostratigraphy provides a detailed age model for the Baskil section due to the continuous, undisturbed, and undeformed sedimentary record [33]. Paleomagnetic analyses resulted in twelve magnetozones that were correlated to the geomagnetic polarity timescale (GPTS) of [44]. The interval here investigated span from middle C19r to the lowermost part of C18n.1n (Figure 2). [PERSON] et al. [3] published oxygen and carbon stable isotopes on benthic (_Cilicidoides_) and planktic (_Acarinina_ and _Subbotinia_) foraminifera that well constrain the MECO isotopic signatures (Figure 2). In addition, detailed mineralogic data to unravel climate changes have been provided by [PERSON] et al. [32] (Figure 2). Fossil assemblages [32; 33; 42] show that the Baskil section cover the top of NP15 to the base of NP18 of calcareous nanofossil zonation of Martini [34]; CP14a to CP15 zonation of Okada and Bukry [35]; MNP16A to MNP18B of [PERSON] et al. [36]; CNE13 to CN18 of [PERSON] et al. [37]; SBZ16/17-SBZ18A of [PERSON] and Ozcan [40]. Planktic foraminifera assem  
Figure 2: Magnetobiostrigraphy, lithological log, and stable isotopes curves of the Baskil section from [3; 33]. Calcareous nannofossil zones and subzones after [34] (listed as NP), [35] (listed as CP), [36] (listed as MNP), and [37] (listed as CNE). Planktic foraminiferal zones are after [38] (listed as E). Larger benthic foraminiferal zones and subzones are after [39; 40]. Carbon (8°13C) and oxygen (8°18O) isotopes are shown for three individual genera of foraminifera, representing surface (_Acarinina_), thermocline (_Subbotinia_) and bottom (_Cibicidoides_) conditions. Diamonds represent individual data points, whereas solid lines represent curves smoothed by three-point-moving average. The record of elements, bulk mineralogy and clay minerals is from [32]. The colored bands highlight the five identified phases. blages indicate that the section spans the (undifferentiated) E10/E11 to E14 biozonations of [PERSON] et al. [38]. These data were used to integrate the age model calculated from the magnetostratigraphy. The Baskil section displays one of the best-preserved records of the MECO event [3]. It yielded \(\delta\)18O and \(\delta\)13C values from different foraminiferal genera representing the bottom, thermocline, and surface environments, which show that the MECO perturbation was recorded at all depths (Figure 2). The isotope curves correlate well with those recorded in other oceanic basins, despite the generally lower values that may be attributed to the local conditions of the Baskil setting [3].