Abstract

Mesopelagic prokaryotes (archaea and bacteria), which are transported together with nutrient-rich intermediate-water to the surface layer by deep convection in the oceans (e.g., winter mixing, upwelling systems), can interact with surface microbial populations. This interaction can potentially affect production rates and biomass of surface microbial populations, and thus play an important role in the marine carbon cycle and oceanic carbon sequestration. The Eastern Mediterranean Sea (EMS) is one of the most oligotrophic and warm systems in the world’s oceans, with usually very shallow winter mixing (<200 m) and lack of large-size spring algal blooms. In this study, we collected seawater (0-1500 m) in 9 different cruises at the open EMS during both the stratified and the mixed seasons. We show that the EMS is a highly oligotrophic regime, resulting in low autotrophic biomass and primary productivity and relatively high heterotrophic prokaryotic biomass and production. Further, we simulated deep water mixing in on-board microcosms using Levantine surface (LSW, ~0.5 m) and intermediate (LIW, ~400 m) waters at a 9:1 ratio, respectively and examined the responses of the microbial populations to such a scenario. We hypothesized that the LIW, being nutrient-rich (e.g., N, P) and a ‘hot-spot’ for microbial activity (due to the warm conditions that prevail in these depths), may supply the LSW with not only key-limiting nutrients but also with viable and active heterotrophic prokaryotes that can interact with the ambient surface microbial population. Indeed, we show that LIW heterotrophic prokaryotes negatively affected the surface phytoplankton populations, resulting in lower chlorophyll-a levels and primary production rates. This may be due to out-competition of phytoplankton by LIW populations for resources and/or by a phytoplankton cell lysis via viral infection. Our results suggest that phytoplankton in the EMS may not likely form blooms, even after exceptionally deep winter mixing, and therefore have a very small overall effect on the vertical flux of organic matter to the deep sea.

Highlights

  • Vast regions of the oceans are considered nutrient-limited and are characterized by low rates of new production and an overall low phytoplankton/microbial biomass

  • Seawater was sampled at discrete depths between the surface (∼0.5 m) and the bottom (∼1,500 m) using Niskin bottles (8 L) mounted on a rosette equipped with a Conductivity Temperature Depth (CTD) sensor (Seabird 19 Plus), a fluorometer (Turner designs, Cyclops-7) and an oxygen optode (Seabird SBE 63)

  • Addition of limiting nutrients to surface waters during winter mixing (Lindell and Post, 1995; Behrenfeld, 2010), upwelling gyres (Groom et al, 2005; Rahav et al, 2013a), coastal upwelling systems (Anabalón et al, 2016), or following external nutrient inputs (Mills et al, 2004; Paerl et al, 2011; Rahav et al, 2016a), often results in phytoplankton blooms (Moore et al, 2013; Rahav and Bar-Zeev, 2017). While this phenomena occurs in most marine environments (Smayda, 1997), phytoplankton blooms rarely occur in the Eastern Mediterranean Sea (EMS) (Groom et al, 2005), despite the fact that deep water mixing (>450m) that replenish the surface water with N and P has been observed in extremely cold winters (Brenner et al, 1991; Krom et al, 1992; Zohary et al, 1998)

Read more

Summary

Introduction

Vast regions of the oceans are considered nutrient-limited and are characterized by low rates of new production and an overall low phytoplankton/microbial biomass. It has been accepted that nutrient availability plays a key role in controlling the marine phytoplankton/microbial biomass, diversity and activity (Arrigo, 2005; Shi et al, 2012). This determines to a great extent the drawdown potential of atmospheric CO2 by the oceanic biological pump and final carbon sequestration in the deep ocean water masses and sediments (Falkowski, 1997; Raven and Falkowski, 1999; Sisma-Ventura et al, 2016). Compared to the nutrient-poor photic layer (0– 150 m), N and P levels in the aphotic layers are 2–3 orders of magnitude higher (Tanhua et al, 2013; Kress et al, 2014)

Methods
Results
Discussion
Conclusion
Full Text
Published version (Free)

Talk to us

Join us for a 30 min session where you can share your feedback and ask us any queries you have

Schedule a call