This is caused by the Phyt decrease due to mortality and Zoop grazing. The larger concentrations of POC calculated for successive decades are reflected by the increased primary production in 2010 as compared to the average in 1965–1998. This, of course, leads to larger DetrP and Zoop concentrations, both contributing to POC. The POC increase is even more pronounced. An interesting shift in the cycles can be noticed towards 2050: a large zooplankton peak develops in October, which leads to a rapid decrease in phytoplankton and detritus in October and November. Zoop, however, gains in importance as a component of POC, giving rise to an extended POC

concentration peak between August and early October. As a consequence, a POC concentration between 900 and 1000 mg m−3 persists between April and October with just a three-week DNA Damage inhibitor long break in July. The cycles of POC itself and POC components are different in BD (Figure 3).

For one thing POC levels are lower: primary production is lower because of the limited supply of nutrients (Renk 2000). Zooplankton thus never develops into a major component of POC, and both Phyt and DetrP concentrations decrease slowly in the autumn. This leads to a gradual decrease in POC concentration by 25% in September/October and by 20% in October/November. Yet another POC cycle characterizes the Gotland Deep. The primary productivity peak begins in April/May. There is no zooplankton that could modify Phyt and DetrP, so POC consists of Phyt and DetrP, the latter derived check details from phytoplankton. Metalloexopeptidase There is just one POC peak, occurring in June (1965–1998) and July (2050). Because of the slow growth of zooplankton in August and September (both 1965–1998 and 2050), phytoplankton and detritus levels fall slowly, leading to a gradual decrease

in POC. The varying patterns and levels of POC in the three deeps are best visualized in Figures 3 and 4, which show monthly and seasonal averages of POC. In GdD elevated POC concentrations from 400 mgC m−3 (2010) to 900 mgC m−3 (2050) in spring are evident. Moreover, the monthly averages for August and September 2050 exceed those of April and May 2050, whereas in 1965–1998 the August and September averages are lower than those for April and May by some 25%. Another difference in the pattern – the greater contribution of the zooplankton biomass to POC in August and September – is also evident (Figure 2). Zooplankton growth leads to a third effect – a rapid decrease in POC concentrations: by 50% in November 2050 but by just 20% in November 1965–1998. This difference is caused by the rapid decline in both Phyt and DetrP due to zooplankton feeding on the other two POC components. Increased temperature and light will prolong the growing season in 2050.