Northward flows were dominant

from January until the middle of February, resulting in a 15 km3 water transport from the Gulf of Riga to the Väinameri. From mid-February until late April, the cumulative water exchange through the Suur Strait was small, although the instantaneous velocities were not. From May till mid-June outflow from the Väinameri to the Gulf of Riga was dominant, the corresponding cumulative water exchange being 10 km3. From May to July the currents were less variable than during the rest of the year. During the summer months (June, July, August) the periods of outflow from the Gulf of Riga alternated with inflow. From October until the end of December there was a gross outflow from check details the Gulf of Riga to the Väinameri: the corresponding cumulative water exchange was approximately 20 km3. The annual water exchange was about 23 km3 from the Gulf of Riga to the Väinameri. To conclude, both the flow speed and the water exchange are characterized by considerable variability. A dominant outflow from the Gulf of Riga to the Väinameri from late autumn to early spring is characteristic of mild winters (Otsmann et al. 2001). For instance, the winter of 1994/1995 was stormy and ice free, which resulted in a strong outflow into the Suur Strait. October–December 1996 was also windy, resulting in a persistent outflow. In contrast, the winter of 1995/1996 was cold (ice cover

in the Suur Strait) and the Pexidartinib research buy dominant winds blew from the north. Under these conditions a weak inflow to the Gulf of Riga through the Suur Strait was observed. 1. Field measurements showed a certain asymmetry between along-strait wind forcing, Cyclin-dependent kinase 3 flow speed and significant wave height. Because of the longer fetch of southerly waves, the highest significant wave heights (maximum 1.6 m) were observed during southerly wind events. Further studies are needed to quantify material transport

through the Suur Strait focusing on the cycling of material between sediments and water. We thank the anonymous referees for their valuable comments on the manuscript. “
“The North Aegean Sea is a part of the Aegean Sea (Figure 1) experiencing complex bathymetric and hydrographic conditions (Lykousis et al. 2002). The bottom topography is characterized by a NE-SW oriented deep trough, separated by shallow sills and shelves, constituting the ‘North Aegean Trough’ (Poulos et al. 1997). Within this trough, three main depressions exist: the Lemnos Basin to the north-east (maximum depth 1470 m), the Athos Basin at the centre (maximum depth 1150 m) and the North Sporades Basin to the south-west (maximum depth 1500 m). A series of shallow sills separate these basins from the Skyros Basin to the south (maximum depth 1077 m), and from the Chios Basin to the west and south of Chios Island, with a maximum depth of 1200 m (Velaoras & Laskaratos 2005).