Baltic Sea

and Hoburg (HB), with positions shown in Fig. 4.28. Both wind series were rotated by 180 ◦
to match the currents, i.e now a positive wind is travelling in an eastward direction and a negative
in a westward direction. Finally the resulting averaged wind components were rotated
anticlockwise by 38 ◦ to obtain the forcing parallel to the main axis of the Baltic Proper.
The wind's eect on well mixed and also stratied elongated basins was extensively studied
by Csanady (1973), Bennett (1974), Krauss (1979), Krauss and Brügge (1991),
Fennel (1986) and Winant (2004) for comparable basins like the Great Lakes as well as
coastal upwelling regions. Their main ndings provide the base for the following discussion on
obtained results from the Stolpe Channel: The surface layer responds with an Ekman transport
10
5
38 (m/s)
0
5
10
A
30/09 10/10 20/10 30/10 09/11 19/11 29/11 09/12 19/12
Date in 2006 (dd/mm)
Depth (m)
ADCP SFN alongslope current [cm/s]
50
45
40
30
50
20
10
55
0
60
10
20
65
30
40
70 50
30/09 10/10 20/10 30/10 09/11 19/11 29/11 09/12 19/12
B
Depth (m)
ADCP SFS alongslope current [cm/s]
50
45
40
30
50
20
10
55
0
60
10
20
65
30
40
70 50
30/09 10/10 20/10 30/10 09/11 19/11 29/11 09/12 19/12
Date in 2006 (dd/mm)
C
Figure 4.27: A: Daily wind u rotated by 38 ◦ and averaged between Arkona and Hoburg. Daily alongslope
current velocities for SFN (Fig. 4.27 B) and SFS (Fig. 4.27 C). Positive values in A, B and C depict
eastward directions, negative values westward directions.
86