In the growing season fresh,

labile organic matter is supplied to the system. This increases concentrations of organic matter (average values for the growing season are: surface DOC ~ 5.0 mg dm− 3; sub-halocline DOC ~ 4.1 mg dm− 3; surface POC ~ 0.9 mg dm− 3, subsurface POC ~ 0.2 mg dm− 3) with labile substances ( Table 4). As soon as the supply is terminated, the labile organic matter is mineralised. This leaves the pool of resistant organic matter in the period late November–mid–April. Then the cycle commences again. The seasonal dynamics of both DOC and POC concentrations (based on Gdańsk Deep results) is quite well developed, as can be seen in Figure 4. DOC and POC profiles (Figure 4) indicate (in the surface layer): residual (DOC: 3.4 mg dm− 3; POC: 0.1 mg dm− 3) RG7422 solubility dmso concentrations in March; the highest concentrations (close to 6.5 mg dm− 3 – DOC; and 1 mg dm− 3 – POC) in May and again smaller concentrations (DOC: 4.5 mg dm− 3; POC: 0.2 mg dm− 3) in October. The March vertical DOC and POC profiles

show the smallest concentrations and almost no vertical gradient. This can be attributed to the lack of biological activity (the temperature at the time of sampling was in the range 3–5 °C). Stable concentrations in the surface water layer can be explained as resulting from intensive vertical mixing, www.selleckchem.com/products/SB-431542.html while low concentrations in the sub-halocline layer can be explained by small DOC and POC concentrations in the North Sea water that had entered the Baltic and had formed the dense, sub-halocline water layer (Thomas et al., 2005 and Maar et al., 2011). DOC and POC Adenosine triphosphate concentrations in May are much larger throughout the water profile, with high concentrations in the surface layer caused by phytoplankton activity and freshwater runoff rich in organic matter. The increase of both DOC and POC concentrations between March and May clearly shows that the fresh dissolved and suspended organic matter, originating from biological activity and river runoff, substantially increase DOC and POC concentrations. The decrease in DOC and POC concentrations

from May to October and from the surface downwards to the bottom are the result of decreased phytoplankton activity – the dominant source of organic carbon in seawater (Hagström et al. 2001). Similar profiles and dependences that lead to the same conclusions were observed in the Gotland Deep and the Bornholm Deep. Obviously, there are numerous factors that influence the intensity and timing of carbon sources and sinks in the course of a year. Thus, it is difficult to expect seasonal fluctuations of both DOC and POC that begin and terminate precisely at the same time. This variability is illustrated by the data presented in Figure 5. Nevertheless, the strong seasonal dependence of carbon concentrations is evident. Seasonal changes are best developed in the case of POC concentrations in the surface water layer (Figure 5). Few changes are observed in the sub-halocline layer.