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Linking ocean biogeochemical cycles and ecosystem structure and function: results of the complex SWAMCO-4 model
Pasquer, B.; Laruelle, G.; Becquevort, S.; Schoemann, V.; Goosse, H.; Lancelot, C. (2005). Linking ocean biogeochemical cycles and ecosystem structure and function: results of the complex SWAMCO-4 model. J. Sea Res. 53(1-2): 93-108. https://dx.doi.org/10.1016/j.seares.2004.07.001
In: Journal of Sea Research. Elsevier/Netherlands Institute for Sea Research: Amsterdam; Den Burg. ISSN 1385-1101; e-ISSN 1873-1414, meer
Ook verschenen in:
Veldhuis, M.J.W. (Ed.) (2005). Iron resources and oceanic nutrients: advancement of global environmental simulations. Journal of Sea Research, 53(1-2). Elsevier: Amsterdam. 120 pp., meer
Peer reviewed article  
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Trefwoorden
    A, North Atlantic
    AE, North Atlantic
    Algae > Diatoms
    AN, North Atlantic
    Antarctic Ocean
    Antarctica
    Aquatic communities > Plankton > Phytoplankton
    AS, North Atlantic
    ASW, North Atlantic
    AW, North Atlantic
    Chemical elements > Metals > Transition elements > Heavy metals > Iron
    Cycles > Chemical cycles > Geochemical cycle > Biogeochemical cycle
    Cycles > Chemical cycles > Geochemical cycle > Biogeochemical cycle > Nutrient cycles > Carbon cycle
    Cycles > Chemical cycles > Geochemical cycle > Biogeochemical cycle > Nutrient cycles > Nitrogen cycle
    Energy transfer
    Hydrographic features > Marine areas > Oceans > Marine areas > Antarctic ocean
    Models
    Bacillariophyceae [WoRMS]; Phaeocystis Lagerheim, 1893 [WoRMS]; Phaeocystis Lagerheim, 1893 [WoRMS]; Prymnesiophyceae [WoRMS]
    Antarctica [Marine Regions]; Noord Atlantisch [Marine Regions]; North Atlantic Ocean [Marine Regions]; North Atlantic Ocean [Marine Regions]; North Atlantic Ocean [Marine Regions]; North Atlantic Ocean [Marine Regions]; North Atlantic Ocean [Marine Regions]
    Marien/Kust
Author keywords
    ecological modelling; diatoms; pico; nanophytoplankton; coccolithophorids; Phaeocystis spp.; iron; air-sea CO2<; sub> fluxes; global ocean; antarctic ocean; North Atlantic
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Abstract
    We present results obtained with SWAMCO-4, a complex model of the marine planktonic system calculating C, N, P, Si, Fe cycling within the upper ocean, the export production and the exchange of CO2 between the ocean and atmosphere. The model, constrained by physical, chemical and biological (grazing, lysis) controls, explicitly details the dynamics of four relevant phytoplankton functional groups with respect to C, N, P, Si, Fe cycling and climate change. Those are diatoms, pico/nano phytoplankton, coccolithophorids, and Phaeocystis spp. whose growth regulation by light, temperature and nutrients has been obtained based on a comprehensive analysis of literature reviews on these taxonomic groups. The performance of SWAMCO-4 is first evaluated in a 1D physical frame throughout its cross application in provinces with contrasted key species dominance, export production, CO2 air-sea fluxes and where biogeochemical time-series data are available for model initialisation and comparison of results. These are: (i) the ice-free Southern Ocean Time Series station KERFIX (50°40S, 68°E) for the period 1993-1994 (diatom-dominated); (ii) the sea-ice associated Ross Sea domain (Station S; 76°S, 180°W) of the Antarctic Environment and Southern Ocean Process Study AESOPS in 1996-1997 (Phaeocystis-dominated); and (iii) the North Atlantic Bloom Experiment NABE (60°N, 20°W) in 1991 (coccolithophorids). We then explore and compare the ocean response to increased atmospheric CO2 by running SWAMCO-4 at the different locations over the last decade. Results show that at all tested latitudes the prescribed increase of atmospheric CO2 enhances the carbon uptake by the ocean. However, the amplitude of the predicted atmospheric CO2 sinks displays large regional and interannual variations due to the actual meteorological forcing that drives the local hydrodynamics. This is particularly true in the marginal ice zone of the Ross Sea (AESOPS) where the magnitude of the predicted annual CO2 sink is positively related to the length of the surface ocean ice-cover period which determines the iron surface concentration at the time of ice melting.
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