The beginning of GI-1 in the Greenland Ice Core record is centred at 14,692 b2k and shows a temperature amplitude increase of 10 °C over just a few years (Blockley et al., 2012b). A warming trend was noticed throughout CEE about the same time (Table 2); however, the timing and magnitude of this EPZ004777 warming can only be roughly estimated (Fig. 2). For example in Slovenia, the δ18O on bulk carbonates from lake sediments indicates a sharp increase in summer temperatures at 14.8 ka cal BP, followed by relatively stable conditions (Andri? et al., 2009). Similarly, a rapid warming phase initiated at ∼14.8 ka cal BP is revealed by the δ18O values of a speleothem from NW Romania (T?ma? et al., 2005) and was also inferred from the growth intervals of another speleothem in Sc?ri?oara Ice Cave (Onac, 2001). For the same region, Feurdean et al. (2008a) used pollen to document a 2 °C increase (from 2 to 4 °C) in annual temperatures that correlate well with the timing of the GS-2/GI-1e transition in Greenland, increase generated by winter temperatures only (summer temperatures remained unchanged). A chironomid-based reconstruction of summer temperatures in the S Romanian Carpathians indicates an increase of ∼2.8 °C in summer air temperature during the same transition, reaching a interferons maximum of ∼8.1 °C (Tóth et al., 2012). Further to the NE during the same period, July temperatures fluctuated between 12 and 16 °C in central Poland (Ralska-Jasiewiczowa et al., 1998; pollen data), 13–16.5 °C at ?abieniec bog, central Poland (P?óciennik et al., 2011; chironomid assemblages) and 15.5–16.5 °C at Lake Okunin, in NW Ukraine (Dobrowolski et al., 2001; ostracod assemblages). In the eastern Baltic area, July temperatures below 12 °C (Kirilova et al., 2011 – chironomid data; Veski et al., 2012; pollen data) were characteristic during the early phase of the Lateglacial (roughly overlapping with GI-1e in Greenland).
↧