Of these, the NCEP-CFSR model detects only Lake Ladoga, presumably because of the sparser resolution of the model. The diurnal evolution of PW, with a 6-hour time step, is shown in Figure 3. At night, from 00 to 06 UTC, there is no change

in PW above the sea, but a decrease above the land is detectable. In the morning, from 06 to 12 UTC, PW decreases above the sea, but increases above the land, especially to the east of the Baltic Sea. In the afternoon, from 12 to 18 UTC, PW still decreases slightly above the water, except in the Gulf of Finland and on Lake Ladoga, where PW is already increasing, as is the case to the west of the Baltic Sea. In the evening, from 18 to 00 UTC, PW is increasing above the water, but PD-0332991 ic50 is mostly decreasing above the land. For the sake of comparison with previous studies (Bouma and Stoew, 2001 and Jakobson et al., 2009), shorter periods were also processed, but because of the insufficient number of data, the diurnal differences remained mostly insignificant (not shown), without any justifiable opportunity for making comparisons. To estimate the influence of different atmospheric layers on PW diurnal variation, the PW difference

between 18 and 06 UTC (dPW = PW18 UTC − PW06 UTC) was calculated, as this time interval usually gives the largest differences in PW. After that, the contributions to dPW from vertical intervals 900–1000 hPa, 800–900 hPa and 800–1000 hPa were calculated (Figure 4). Lower 100 hPa humidity diurnal variations affect PW diurnal variability more above the water than the land, while the 800 to 900 hPa interval affects it more above land than the water. Relatively speaking, ITF2357 nmr the regional average contribution to dPW was 25% in the interval 900–1000 hPa and 45% in the next 100 hPa layer. The 800–1000 hPa interval holds 70% of the dPW with a ca 20% larger contribution above the land than over the sea. Specific humidity

and temperature at 00, 06, 12 and 18 UTC differ from their diurnal average values at different vertical pressure levels and exhibit fundamental differences for the sea and the land (Figure 5). The results for BaltAn65 + and NCEP-CFSR (not Resveratrol shown) were similar at all vertical levels with respect to both specific humidity and temperature. The behaviour of specific humidity above 950 hPa is the reverse of that above the sea and the land. Above the sea there is less humidity at 12 and 18 UTC, while above the land the humidity is lower at 00 and 06 UTC. The situation regarding the specific humidity below 950 hPa is more complicated and will be analysed in the Discussion. Over land, temperatures are higher at 18 and 12 UTC and lower at 06 and 00 UTC. Diurnal variability in the temperature above the water is delayed for about 6 hours, compared to the variability above the land, with higher temperatures at 18 and 00 UTC and lower temperatures at 06 and 12 UTC, although the delay fades out above 850 hPa.