Abstract
The distribution and variability of phytoplankton in the upper layers of the ocean are highly correlated with physical processes at different time and spatial scales. Model simulations have shown that submesoscale features play a pivotal role on plankton distribution, metabolism and carbon fluxes. However, there is a lack of observational studies that provide evidence for the complexity of short-term phytoplankton distribution and variability inferred from theoretical and modeling approaches. In the present study, the development and decay of a submesoscale front south of Gran Canaria Island is tracked at scales not considered in regular oceanographic samplings in order to analyze the picoplankton response to short-term variability. Likewise, the contribution of each scale of variability to the total variance of the picophytoplankton community has been quantified. We observe statistically different picophytoplankton assemblages across stations closer than 5 km, and between time periods shorter than 24 h, which were related to high physical spatiotemporal variability. Our results suggest that both temporal and spatial variability may equally contribute to the total variance of picoplankton community in the mixed layer, while time is the principal contributor to total variance in the deep chlorophyll maximum (DCM).
Highlights
IntroductionUnicellular marine primary producers’ growth mainly depends on nutrient and light availability
As higher plants, unicellular marine primary producers’ growth mainly depends on nutrient and light availability
We considered that Pro and NOx− maximums resemblance seems to be a coincidence rather than a causality, and that front-driven accumulation of dissolved organic matter (DOC) would be the reason of high abundances of Pro at nutrient upwelling stations
Summary
Unicellular marine primary producers’ growth mainly depends on nutrient and light availability. Intensification of diapycnal mixing may enhance vertical transport of nutrients (Arcos-Pulido et al, 2014; Corredor-Acosta et al, 2020; Tsutsumi et al, 2020) as well as upwelling/downwelling of phytoplankton communities from sub-surface layers into the euphotic zone and vice versa. These physical cells act to restore the geostrophy by means of restratification in a process known as frontogenesis (Hoskins and Bretherton, 1972; Hoskins, 1982; Capet et al, 2008; McWilliams, 2016). Submesoscale motions may induce shifts on phytoplankton community structure (D’Ovidio et al, 2010; Lévy et al, 2018) affecting food web dynamics and, the carbon cycle (Mayot et al, 2017)
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