In the Irminger Sea, the long-term freshening in the deep water column
(σ 0 > 27.80, depths >∼ 2000 m) reversed in the early 2000s [17]. The observed
freshening reversal was a lagged consequence of the persistent ISOW salinification
Fig. 2 Oxygen concentrations (ml/l) in the water column (lower panel) as observed in March–
October 1997 in four hydrographic sections (upper panel) ending nearby the southern tip of
Greenland. A separate oxygen maximum in the (LSW) layer (1000–2000 m) in the Irminger Sea at
59.5° N strongly implies local convective renewal of LSW before 1997.
Adapted from [13]
Fig. 3 Warming and salinification in the northern North Atlantic between the mid-1990s and
mid-2000s, as observed at 59.5° N. The figure shows the 2006–1997 temperature (°C, left) and
salinity (right) differences on isobaric surfaces in the Irminger Sea and Iceland Basin.
Adapted from [15]
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A. Sarafanov et al.
(σ 0 > 27.80, depths >∼ 2000 m) reversed in the early 2000s [17]. The observed
freshening reversal was a lagged consequence of the persistent ISOW salinification
Fig. 2 Oxygen concentrations (ml/l) in the water column (lower panel) as observed in March–
October 1997 in four hydrographic sections (upper panel) ending nearby the southern tip of
Greenland. A separate oxygen maximum in the (LSW) layer (1000–2000 m) in the Irminger Sea at
59.5° N strongly implies local convective renewal of LSW before 1997.
Adapted from [13]
Fig. 3 Warming and salinification in the northern North Atlantic between the mid-1990s and
mid-2000s, as observed at 59.5° N. The figure shows the 2006–1997 temperature (°C, left) and
salinity (right) differences on isobaric surfaces in the Irminger Sea and Iceland Basin.
Adapted from [15]
418
A. Sarafanov et al.