Moose Project > Biogeochemical cycles EN bis

Biogeochemical cycling and acidification

Biogeochemical cycling of major nutrients is already changing in the Mediterranean Sea.

In the Algero-Provencal basin, the statistical analysis of historical data set of nitrate phosphate and silicic acid concentrations show contrasted trends for the different elements. In the deep water, the silicic acid concentration has remained nearly invariant since the early 1960s. In contrast phosphate and nitrate concentrations increased from the early 1960s and from 1972, respectively. The changes in N and P (0.5% yr-1 between 1960 and 1994) very likely result from anthropogenic activities which translate in a 0.3 % yr-1 increase of the atmospheric and terrestrial inputs of N and P. In contrast, Si input was mainly driven by natural processes. It has been suggested that the increase by a factor 3 of the input of N and P in the Mediterranean Sea has resulted in an increase of new production of 2.7. Consequently the amount of O2 consumed in the deep water to remineralise the exported material could also have increased. The dense water formation is a major process that supplies oxygen to the deep layers. If this process is kept constant, O2 in the deep water might decrease with time and critical values for the benthic fauna might be reached in the middle of the 21century.

How new production and carbon export will change during the next decades in response to the changing nutrient supply? What will be the consequences for the O2 concentration in the deep water?

In the next decade the weakening of the dense water formation is a possible consequence of the climate change in the Mediterranean Sea with two possible antagonist effects on the cycling of the major elements. In the surface waters, the increase in the stratification will reduce the supply of nutrients and will decrease the new production. This process should counteract the predicted increase in new production and in carbon export due to the raising of nutrient terrestrial discharge. In the deep water, the consumption of O2 for the remineralisation could be reduced due to the decrease in carbon export but concomitantly the supply of O2 to the deep water could also be reduced. The net effect on the O2 level in the deep water is difficult to predict.

The nutrient ratio (P:N) in the Mediterranean sea (1:24 in the eastern basin and 1: 22 in the western basin) deviates largely from the canonical values of Redfield. (1:15). Deficit of phosphate (for example due to scavenging by dust) or excess of nitrogen related to efficient dinitrogen fixation by diazotroph organisms have been proposed to explain the high P:N ratio.

The number of studies aiming to quantify the N2 fixation in the Mediterranean sea is growing rapidly, but the exact contribution of this process to the new production and to the N:P ratio has still to be determined. The organisms that are fixing N2 in Mediterranean Sea are not well known. But it is largely recognized that P and Fe are important nutrients for the diazotrophs. Atmospheric deposition is a major mode of supply for both elements (Bonnet and Guieu, 2006; Ridame et al., 2003; Guieu et al. 2002). The nature (anthropogenic versus natural dust) and the magnitude of the atmospheric deposit to the surface waters of the Mediterranean seas are also expected to change during this century (see section WP5). This will impact the nutrient cycling in a way that is actually very difficult to predict.

How will the steochiometry of the major element change?

A long term change of the N:Si:P ratio was also detected in the deep water of the Algero-Provencal basin where the ratio (N:Si:P) increased from 1:24:22 in 1960 to 1:19.5:22 in 2000. The decrease of the ratio Si:P is related to the difference in the time evolution of the supply ; Si was constant whereas P increased. This change may drive important changes in the structure of the phytoplankton community a different levels. A major shift from a diatom to a non diatom dominated system but also more subtle changes within the specific composition of the diatom community are possible. These shifts might favour episodic blooms of toxic phytoplankton species, promote shifts in the composition of the zooplankton community but also in return modify the cycling of the nutrients (Béthoux et al., 1990, 2002; Roether et al., 1998; Tsimplis and Baker, 2000)