Abstract

Diatom production is mainly supported by the dissolution of biogenic silica (bSiO2) within the first 200 meters of the water column. The upper oceanic layer is enriched in dissolved and/or colloidal organic matter, such as exopolymeric polysaccharides (EPS) and transparent exopolymeric particles (TEP) excreted by phytoplankton in large amounts, especially at the end of a bloom. In this study we explored for the first time the direct influence of TEP-enriched diatom excretions on bSiO2 dissolution. Twelve dissolution experiments on fresh and fossil diatom frustules were carried out on seawater containing different concentrations of TEP extracted from diatom cultures. Fresh diatom frustules were cleaned from the organic matter by low ash temperature, and fossil diatoms were made from diatomite powder. Results confirm that newly formed bSiO2 dissolved at a faster rate than fossil diatoms due to a lower aluminium (Al) content. Diatom excretions have no effect on the dissolution of the newly formed bSiO2 from Chaetoceros neogracile. Reversely, the diatomite specific dissolution rate constant and solubility of the bSiO2 were positively correlated to TEP concentrations, suggesting that diatom excretion may provide an alternative source of dSi when limitations arise.

Highlights

  • The terrestrial lithosphere is composed of 27% silicon

  • This increase was steeper for freshly cleaned diatoms than for fossil diatoms

  • The main goal of this study was to understand the influence of transparent exopolymeric particles (TEP) on biogenic silica dissolution

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Summary

Introduction

The terrestrial lithosphere is composed of 27% (by weight) silicon. As a nutrient and required element of various marine organisms, silicon has an important part in biogeochemical processes. Diatoms (Bacillariophyceae), unicellular phytoplankton with an absolute requirement for silicon to build their frustules composed of amorphous polymerised silica (bSiO2), are key silicifying organisms that play an important role in the marine biogeochemical cycling of carbon. They are responsible for nearly 40% of the global primary production (Nelson et al, 1995; Rousseaux and Gregg, 2013). This contribution to the carbon cycle varies greatly according to the oceanic region and period of the year.

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