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47
°N
46
45
44
43
22-GC3/8
42
Sofular Cave
Bosporus
24-GC3
41
40
27
°E
28
29
30
31
32
33
34
35
36
37
38
39
40
41
42
Fig. 1 Location of Sofular cave in northwestern Turkey and of the sediment cores 22-GC3/8 and
24-GC3 in the southeastern Black Sea
depositional environment (Nowaczyk et al.
2012
). The stable oxygen isotope
composition determined on ostracod shells indicates major hydrographic changes in
the basin and was used for stratigraphic purposes. Palynological analyzes were used
to evaluate vegetation changes in the hinterland (Shumilovskikh et al.
2012
) while
dino
agellate cyst concentrations were used as proxy for changes in aquatic primary
productivity and cyst composition for reconstructing surface salinity and tempera-
ture (Shumilovskikh et al.
2013a
). The stratigraphy of the cores includes radiocarbon
dates, tephra dates, paleomagnetic records, correlations of the
fl
18
O ostracod/bivalve
δ
18
O speleothem record from Sofular Cave,
record with the uranium-series dated
δ
18
O NGRIP ice core record, and palynological
correlations to pollen records from the Mediterranean region (Nowaczyk et al.
2012
;
Shumilovskikh et al.
2012
,
2013a
).
proxy matching to the Greenland
δ
3 Key Findings
The last two glacial terminations and subsequent interglacial periods (Holocene and
Eemian) show largely similar patterns of environmental transitions in Northern
Anatolia and the southern Black Sea (Fig.
2
). Disconnected from the Mediterranean
Sea, the Black Sea was characterized by freshwater/brackish dinocyst assemblages
during the ending glacials and abundant IRD suggesting coastal ice formation during
extreme winters (Fig.
2
e,f; Nowaczyk et al.
2012
; Shumilovskikh et al.
2012
,
2013a
).
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