D. Zúñiga1,2,3*
A. Sanchez-Vidal4
M. M. Flexas5
D. Carroll6
M. M. Rufino2,7
G. Spreen8
A. Calafat4
F. Abrantes2,3- 1Instituto de Investigacións Mariñas, Spanish National Research Council (CSIC), Vigo, Spain
- 2Div. Geologia e Georecursos Marinhos, Portuguese Institute for the Sea and Atmosphere (IPMA), Lisbon, Portugal
- 3CCMAR - Centre of Marine Sciences, University of Algarve, Faro, Portugal
- 4GRC Geociències Marines, Universitat de Barcelona, Barcelona, Spain
- 5California Institute of Technology, Pasadena, CA, United States
- 6Moss Landing Marine Laboratories, San José State University, Moss Landing, CA, United States
- 7CEAUL, Centre of Statistics and its Applications, Faculty of Sciences, University of Lisbon, Lisbon, Portugal
- 8Institute of Environmental Physics, University of Bremen, Bremen, Germany
Physical and biogeochemical processes in the Southern Ocean are fundamental for modulating global climate. In this context, a process-based understanding of how Antarctic diatoms control primary production and carbon export, and hence global-ocean carbon sequestration, has been identified as a scientific priority. Here we use novel sediment trap observations in combination with a data-assimilative ocean biogeochemistry model (ECCO-Darwin) to understand how environmental conditions trigger diatom ecology in the iron-fertilized southern Scotia Sea. We unravel the role of diatoms assemblage in controlling the biogeochemistry of sinking material escaping from the euphotic zone, and discuss the link between changes in upper-ocean environmental conditions and the composition of settling material exported from the surface to 1,000 m depth from March 2012 to January 2013. The combined analysis of in situ observations and model simulation suggests that an anomalous sea-ice episode in early summer 2012–2013 favored (via restratification due to sea-ice melt) an early massive bloom of Corethron pennatum that rapidly sank to depth. This event drove high biogenic silicon to organic carbon export ratios, while modulating the carbon and nitrogen isotopic signals of sinking organic matter reaching the deep ocean. Our findings highlight the role of diatom ecology in modulating silicon vs. carbon sequestration efficiency, a critical factor for determining the stoichiometric relationship of limiting nutrients in the Southern Ocean.
Introduction
The Southern Ocean (SO) is one of the most productive regions in the global ocean, and through its connection with all other basins, has sparked intense debate of how this remote region modulates global climate (Falkowski et al., 1998; Sarmiento et al., 2004). In this context, phytoplankton are of utmost importance due to their critical role in ocean carbon sequestration. These tiny organisms are fundamental for modulating climate change through their capacity to consume and export atmospheric carbon dioxide (CO2) to bottom sediments (Smetacek et al., 2012; Boyd et al., 2016; Tréguer et al., 2017). Furthermore, phytoplankton in the SO may influence productivity at global scales by modifying the stoichiometric relationships of SO nutrients that are transported to distant regions around the global ocean (Pondaven et al., 2000; Ragueneau et al., 2000; Brzezinski et al., 2002; Matsumoto and SarmientoBrzezinski, 2002).
While the phytoplankton community varies between different SO biogeochemical provinces, there is clear consensus that diatoms, which are unicellular organisms with silica skeletons, are the dominant phytoplankton group during elevated primary productivity events (Bathmann et al., 1997; Arrigo et al., 1999; Landry et al., 2002). In the remote SO, where macronutrients remain high, dissolved iron (dFe) content in combination with light availability acts as the limiting factor for diatom growth (Martin et al., 1990; Buma et al., 1991; Boyd et al., 2007). Furthermore, dFe variability can also shift diatoms community structure, through the promotion of different physiological and survival strategies (Hutchins and Bruland, 1998; Takeda, 1998; Marchetti and Cassar, 2009; Quéguiner, 2013). The largest ecological manipulation experiment to date in the SO revealed that Fe addition promoted thin-shelled small diatoms, while Fe-limited conditions led to the dominance of heavily-silicified diatoms (Assmy et al., 2013). While the results from this groundbreaking experiment provide invaluable information linking diatom ecology to SO biogeochemistry, other critical aspects, such as how other environmental factors (e.g., irradiance, temperature, and water column stability) control the diatom species succession remain poorly understood (Boyd, 2013).
Due to their high sinking rates, diatoms have the capacity to transfer organic carbon (OC) and biogenic silicon (bioSi) from the productive surface layer to the deep ocean. As a result, diatoms are widely identified as the most relevant phytoplankton group for unraveling SO organic carbon cycling (Bathmann et al., 1991; Smetacek et al., 2012; Krause and Lomas, 2020). To fully understand diatom-driven export, and hence how carbon and silicon are sequestered, it is also critical to consider diatom ecological traits. These traits respond to favorable growth conditions, determine the survival of one species vs. another, and consequently impacts settling velocity. While sinking, the intact survival of diatom frustules depends on the resistance of their siliceous skeletons to dissolution and the impact of remineralization processes on their cell’s organic content. These two aspects, along with the capability of diatoms to avoid grazing by pelagic zooplankton, must be considered for a complete understanding of which diatom species reach the seafloor and impact sediment composition. In this context, studies based on sediment trap data are especially important, since they represent the missing link between processes occurring at the ocean surface and the seafloor. Despite sparse sediment trap observations in the SO, previous in-situ studies have been fundamental for understanding the role of seasonal diatom assemblages in determining the transfer efficiency of biogenic matter escaping the epipelagic domain (Fischer et al., 2002; Pilskaln et al., 2004; Salter et al., 2007; Ichinomiya et al., 2008; Salter et al., 2012; Grigorov et al., 2014; Rembauville et al., 2015; Rigual-Hernández et al., 2015, 2016; Rigual-Hernandez et al., 2019). However, only few studies discuss variability in export rates by considering environmental factors to regulate seasonal diatom production in the upper water column (Salter et al., 2012; Rigual-Hernández et al., 2015, 2019; Rembauville et al., 2018).
In the South Atlantic sector of the SO, naturally Fe-enriched shelf waters from the Antarctic Peninsula meet the southern boundary of the Antarctic Circumpolar Current (Figure 1) (Orsi et al., 1995; Dulaiova et al., 2009; DeJong et al., 2012; Jiang et al., 2019; Sanchez et al., 2019). This leads to relatively high rates of primary production compared to other SO biogeochemical regions (de Baar et al., 1995; Holm-Hansen et al., 2004; Ardelan et al., 2010). Despite their importance in terms of quantifying productivity, previous particle flux studies in this region are scarce and are based on free-drifting traps deployed for short time periods (Bodungen et al., 1986; Gersonde and Wefer, 1987; Abelmann and Gersonde, 1991; Leventer, 1991), which limits our understanding of carbon and silicon sequestration on seasonal and longer timescales.
FIGURE 1. Map of the study region depicting bathymetry, main oceanographic fronts and the sediment trap location (yellow star). ECCO-Darwin dissolved iron concentration (dFe, in color) for the month of December 2012 at 150 m depth shows the supply of dFe from the tip of the Antarctic Peninsula. Antarctic Circumpolar fronts (Orsi et al., 1995) are shown in gray (SAF: Sub-Antarctic front; PF: Polar Front; SACCF: Southern Antarctic Circumpolar Current Front; Bdy: Southern boundary of the Antarctic Circumpolar Current); the Antarctic Slope Front (ASF) is shown in light green; and the outer limit of the Weddell Gyre is indicated with a dashed black line. The zonal band between the southern boundary (Bdy) of the ACC and the northern limit of the Weddell Gyre is known as the Weddell Scotia Confluence (WSC; Patterson and Sievers, 1980). Isobaths are shown as black contours (500 m, thick line; every 1,000 m, thin lines).
The primary goal of this study is to determine the role of diatoms in driving the export of OC and bioSi to depth in the Fe-fertilized southern Scotia Sea by analyzing sinking diatom assemblage, along with isotopic and major element composition of settling particles. These data provide unprecedented detail on: 1) how diatom survival strategies regulate the biogeochemical signature of exported particles and 2) how diatom floristics respond to changing environmental conditions. Our work fills a critical gap in understanding the role of diatom ecology in the SO carbon cycle, while providing novel information on the use of fossil diatom assemblages as a proxy for past primary production. Ultimately, our results provide new insight on the role of diatoms in the biogeochemistry cycle of SO waters.
Data and Methods
Study Region
The study site is located in the Weddell-Scotia Confluence (WSC, Figure 1), a weakly-stratified region with sub-surface temperature and salinity that is lower than waters located to the north and the south (Patterson and Sievers, 1980; Orsi et al., 1993; Whitworth et al., 1994). Relatively warm sub-surface waters in the north (Circumpolar Deep Water, in the Scotia Sea) and the south (Warm Deep Water, in the Weddell Sea) mark the meridional extension of the Confluence Zone. The currents associated with these water masses (the Antarctic Circumpolar Current and the Weddell Gyre) confer a general eastward zonal flow on both limits. The weak stratification of the WSC is caused by strong lateral mixing along isopycnals (Whitworth et al., 1994), and enhanced diapycnal mixing near the bottom (Naveira-Garabato et al., 2002). Rectified tidal flows are responsible for sustaining the Antarctic Slope Front (Jacobs, 1991) over the complex double-ridge topography (Heywood et al., 2004; Flexas et al., 2015). Wind forcing controls the surface circulation over the South Scotia Ridge. In particular, wind stress curl over the Weddell Gyre determines the pathway of surface waters exported into the Scotia Sea (Youngs et al., 2015) and thus has a large impact on surface-ocean chlorophyll patterns in this region (Thompson and Youngs, 2013). Sea ice from the continental shelf and slope of the Weddell Sea is advected by local winds, which also control sea-ice concentration trends (Holland and Kwok, 2012) (Supplementary Figure S1).
Sediment Trap Observations
In the framework of a multi-year international program focused on studying the Antarctic Slope Front over the South Scotia Ridge (Palmer et al., 2012; Flexas et al., 2015), an instrumented mooring with a near-bottom sediment trap (1,000 m depth) was deployed from March 2012 toJanuary 2013 at the northern slope of the South Scotia Ridge (60°S, 53°W; 1,130 m isobath) with sampling periods of one month. Representing dates are referred to the middle point of each sampling period that begins the first day of the corresponding month. The sediment trap was a Technicap PPS3 (0.125 m2 collecting area) with a cylindroconical collection funnel and 12 polypropylene collecting cups, which were set to rotate every month. Before the deployment, the cups were cleaned with 0.5 N HCl, rinsed with ultrapure water, and filled with buffered 5% (v/v) formaldehyde solution in 0.45 µm filtered seawater. After recovery, the closed cups were stored in the dark at 2–4°C until they were processed in the laboratory, within a maximum delay of a few weeks. After decantation of the supernatant, particles were wet-sieved through a 1 mm nylon mesh to retain the largest swimmers, while the smaller ones were removed under a dissecting microscope using fine tweezers. The sample was then divided into 6–12 equal wet aliquots for biogeochemical analyses and diatom identification using a rotary splitting method following the methodology described in Heussner et al. (1990).
The total mass was determined gravimetrically on two or three sub-samples. The replicates were filtered onto cellulose acetate membranes (0.45 μm pore size, 47 mm diameter), rinsed with distilled water to remove salts and excess formalin, and dried to constant weight at 40 C during 24 h. One of the aliquots of each sediment trap sample was freeze-dried, ground and homogenized. Assuming that all the inorganic carbon was constituted by calcium carbonate, the organic matter (organic carbon × 2) and the calcium carbonate [(total carbon–organic carbon) × 8.33] were calculated. The lithogenic (terrigenous) fraction was obtained by the difference between the total mass and the sum of the biogenic compounds [organic matter, calcium carbonate and biogenic silicon (bioSi)].
Total and organic carbon (OC) and total nitrogen (TN) contents, and the stable isotope composition of OC and TN, were measured on an elemental analyzer interfaced to an isotope ratio mass spectrometer at the Scientific and Technological Centers of the University of Barcelona. Samples for OC analysis were first treated with HCl 25% to remove inorganic carbon. The results of isotopic analyses are presented in the conventional δ notation, which is defined as δX = [(Rsample/Rstandard)- 1] x 1,000, where X is 13C or 15N and R is the isotopic ratio of 13C/12C or 15N/14N. Isotopic ratios of the samples (Rsample) are expressed relative to those of a standard (Rstandard), the Pee Dee Belemnite for C and atmospheric N2 for N.
BioSi was analyzed using a two-step extraction with 0.5 M Na2CO3 (2.5 h each) separated after filtration of the leachate. Inductive Coupled Plasma Atomic Emission Spectroscopy (ICP-AES) was used to analyze Si and Al contents in the leachates, and a correction of the Si of the first leachate by the Si/Al relation of the second leachate was applied in order to correct for the excess Si dissolved from aluminosilicates and obtain the bioSi concentration (Kamatani and Oku, 2000). Thus, in this paper we provide bioSi (silicon) strictly speaking, not silica (SiO2) neither amorphous hydrated silica (opal, SiO2 0.4H2O) as reported by Mortlock and Froelich (1989). Dissolved elements in the supernatant overlying the trap particulate samples were not measured and thus particulate fluxes have not been corrected for total fluxes.
Diatom counting and identification was performed using a full sediment trap sample aliquot (Abrantes et al., 2005). Each sample was first cleaned of organic matter and carbonate by additions of H2O2 30% and HCl 10%, respectively. Permanent slides of the entire aliquots (2 fractions <63 µm and >63 µm) were prepared using the evaporation n-tray method (Battarbee, 1973) and the Norland optical adhesive (NOA61) as mounting medium. Diatom counting and species identification was performed at 1000 X (×10 eyepieces and ×100 objectives), using a Nikon Eclipse E100 microscope equipped with Differential Interference Contrast. Exactly 100 randomly-selected fields of view were counted in three replicate slides. For each sample, 300 specimens were identified to the species level and raw counts were then converted to percent abundance. Data presented in this work only includes the dominant diatom species, which represent >70% of the total diatom assemblage.
Sea-Ice Concentrations
Sea-ice velocity fields (Supplementary Figure S1) were obtained from Tschudi et al. (2016). Sea-ice concentration data for years 2012 and 2013 were obtained from the 89 GHz channels of the AMSR2 satellite microwave radiometer with a grid resolution of 6.25 km (Spreen et al., 2008, data available from www.seaice.uni-bremen.de). Sea-ice concentration anomalies (Supplementary Figure S2) were calculated as differences relative to the December 1979–2016 mean sea-ice concentration based on SMMR and SSM/I-SSMIS data at 25 km grid resolution (Cavalieri et al., 2016). The same sea-ice data were also used to calculate sea-ice persistence (Supplementary Figure S3) and the sea ice concentration time series in Figure 2A for a 75 × 81 km region surrounding the mooring.
FIGURE 2. Sea-ice concentration from satellite observations (SSM-I) and environmental variables from ECCO-Darwin at the sediment trap location. (A) Sea-ice concentration, (B) Photosynthethic Active Radiation (PAR, µ Eins m−2 s−1), (C) potential temperature, (D) stratification (-dρ/dz, kg m−4), (E) Chlorophyll a (Chl a, mg m−3), (F) and (G) concentration of dissolved nitrate (NO3, mmol m−3) and dissolved iron (dFe, mmol m−3), respectively. Photic layer depth is shown as gray circles in panels (B) and (E).
ECCO-Darwin
The state-of-the-art ECCO-Darwin ocean biogeochemistry model and its performance has been extensively discussed in the literature (Brix et al., 2015; Manizza et al., 2019; Carroll et al., 2020). ECCO-Darwin is based on a global ocean and sea-ice configuration of the Massachusetts Institute of Technology general circulation model (MITgcm) (Marshall et al., 1997). The physical ocean circulation is from the Estimating the Circulation and Climate of the Ocean (ECCO) consortium (Wunsch et al., 2009), which synthesizes the MITgcm with nearly all available ocean observations since the era of satellite altimetry (∼1992), and provides an adjoint-method-based reconstruction of the three-dimensional, time-varying global ocean and sea-ice state. The ECCO circulation estimates are used to drive an online ecosystem model provided by the MIT Darwin Project (Follows et al., 2007; Follows and Dutkiewicz, 2011; Dutkiewicz et al., 2015), which in turn drives and interacts with marine chemistry variables. ECCO-Darwin uses physical fields from the recently released ECCO LLC270 global ocean and sea-ice data synthesis (Zhang et al., 2018); ECCO LLC270 has ∼18 km horizontal grid spacing at high latitudes.
The MIT Darwin Project ecosystem model is used to couple the ECCO physical solution with ocean ecology and carbon chemistry (Brix et al., 2015; Manizza et al., 2019; Carroll et al., 2020). Standard ecological equations and parameters (Dutkiewicz et al., 2019) are employed; the Darwin ecology includes five large-to-small phytoplankton function types (diatoms, other large eukaryotes, Synechococcus, and low- and high-light adapted Prochlorococcus) and two zooplankton types that graze preferentially on either the large eukaryotes or small picoplankton. Biogeochemical tracers (inorganic nutrients, phytoplankton, zooplankton, dissolved organic matter, and detrital particles) are advected and mixed online by the ECCO LLC270 physical fields. The carbon and nitrogen cycle in Darwin is explicitly represented, along with phosphorus, iron, silicon, oxygen, and alkalinity. To provide an estimate of realistic physical and biogeochemical conditions in the water column we use daily model outputs from January 2012 to March 2013, taken at the grid cell closest to the mooring location.
Statistical Analysis
The relationship between the relative abundance of diatom species assemblages and upper-ocean environmental variables obtained from ECCO-Darwin model during the period March 2012 – January 2013 were analyzed using the ordination technique canonical correspondence analysis (CCA) (vegan package, R-project; ter Braak, 1986; Oksanen et al., 2015).
The water-column environmental data used for this exploration is the result of averaging or integrating each value to the photic layer depth after determining the depth where photosynthetic available radiation (PAR) is 1% of its surface value and above a minimum threshold of 1 µ Ein m−2 s−1 (Table 1).
TABLE 1. Water-column environmental variables obtained from ECCO-Darwin at the mooring location. Daily data were averaged (indicated with *) or integrated within the photic layer depth after determining the depth at which photosynthetic available radiation (PAR) equals 1% of its surface value, and above a minimum threshold of 1 µ Ein m−2 s−1. Data was subsequently averaged over the time interval corresponding to each trap sample (code E1 to E11). PAR: Photosynthethic Active Radiation; MLD, mixed layer depth; Temp, potential temperature; Sal, salinity; Strat, stratification; NO3, nitrate concentration; PO4, phosphate concentration; SiO2, silicate concentration; dFe, total dissolved iron concentration; bioSi/OC, biogenic silicon/organic carbon molar ratio; Chl a, chlorophyll a concentration.
Preliminary variable reduction was carried out through hierarchical cluster analysis using euclidean distance, principal component analysis, and correlation matrix plots, which were used to determine the main groups of variables (not shown for brevity). Within each main group, a representative variable was selected, based on the relationship with other variables and on previous scientific knowledge, to avoid issues with collinearity and for variable reduction. Thus, for the final analysis, sampling time (month), temperature (temp), sea-ice concentration (seaice), dissolved iron (dFe), stratification (strat), particulate organic carbon (POC), Photosynthethic Active Radiation (PAR) and chlorophyll a (chl) were considered. The effect of multicollinearity of environmental variables was checked after modeling using variance inflation factors (VIFs) applied to the CCA. For the species matrix, Hellinger distance was used, as recommended for community compositional data (Legendre and Gallagher, 2001). Significant environmental variables were identified via a stepwise procedure, using permutation tests (999 permutations). After the selection of the significant variables, the model was tested a second time through a Monte Carlo global permutation test (999 permutations) to assess the significance of ordination axes, partial terms and global model.
The results of the CCA are presented as an ordination triplot diagram containing the explanatory variables plotted as arrows along with numbers for samples (dates) and diatom species (main groups of diatoms). All statistical analysis was carried out using r-project (ter Braak, 1986; Oksanen et al., 2015).
Results
Environmental Data and Water-Column Characteristics From ECCO-Darwin
We first use ECCO-Darwin, which provides a best-possible estimate of the global-ocean state by assimilating both physical and biogeochemical observation to infer the environmental conditions and the associated seasonal variability at the mooring location during 2012–2013. Larger concentrations of sea ice were observed in June–July 2012 and in December 2012 (Figure 2A), when sea ice was advected into the study region from the Weddell Sea (Supplementary Figure S1). Sea ice is typically present in the area during austral winter but not in summer. In December 2012 the sea-ice edge was located 200–300 km northward from its typical location, causing the study area to be anomalously covered by 30% sea-ice concentration (Supplementary Figure S2). The sea-ice anomaly was such that in over 38 years of satellite data, sea ice was never observed in the area during December (Supplementary Figure S3).
Sea-ice concentration from ECCO-Darwin showed general agreement with satellite observations (Figure 2A). Upper-ocean properties (surface to 150-m depth) extracted from ECCO-Darwin at the mooring location are shown in Figure 2 and Table 1. Relatively high PAR was observed in austral spring and summer months (January – March 2012, and from October 2012 to January 2013; Figure 2B) due to net heat gain from the atmosphere into the ocean. Mean ocean temperatures within the photic layer ranged between −0.1 and 1.8°C and presented maximum values in concordance with high PAR and absence of sea ice (Figures 2A–C and Table 1). The relatively low stratification increased three-fold in January 2013, due to sea-ice melt (Figure 2D). Spring-summer peaks of Chl a between second half of January–March 2012 and January 2013 were associated with dissolved iron and nitrate consumption by model phytoplankton (Figures 2E–G).
Sinking Particulate Material Time Series
Biosiliceous organism fluxes at 1000-m depth ranged between a maximum of 5.6 106 valves m−2d−1 in June 2012 to a minimum of 2.5 106 valves m−2d−1 in September 2012 (Figure 3A). Diatoms dominated the total siliceous microorganisms during all months, whilst silicoflagellates constitute less than 1% (Figure 3A). Diatom fluxes averaged 3.5 106 valves m−2d−1 and showed marked inter-month variability in terms of assemblage. The large-sized diatom Corethron pennatum (Grunow) Ostenfeld (diameter ∼47 μm; pervalvar axis ∼149 µm) (Annett et al., 2010) and Chaetoceros sp. resting spores were dominant during summer (March 2012 and December 2012–January 2013), reaching up to 67% (January 2013) and 25% (March 2012) of the total flux, respectively (Figures 3B, 4A,D). Thalassiosira gracilis (Karsten) Hustedt became more abundant during winter, representing up to 43% of the total diatom flux in June 2012 (Figures 3B, 4C). The diatom assemblage in sinking particles was also explained by the highly silicified Fragilariopsis kerguelensis (O’Meara) Hustedt (whose relative contribution remained relatively constant throughout the year, ∼26%), the sea-ice related species Fragilariopsis curta (Van Heurck) Hustedt and Fragilariopsis cylindrus (Grunow ex Cleve) Helmcke and Krieger (<7% on average), and the large Oodontellaceae diatom Odontella weissflogii (Grunow) Grunow (reached up to 7%) (Figures 3B, 4B,E,F).
FIGURE 3. Time series for biosiliceous organisms, diatom assemblage and biogeochemical signals of the settling material recovered by a sediment trap at 1,000 m depth in 2012/13. (A) Total biosiliceous (bioSi) organisms. (B) main diatom species abundance. (C) Fluxes of biogenic silicon (bioSi) and organic carbon (OC). (D) OC normalized bioSi molar ratio. (E) Stable isotope ratios of C (δ13OC) and N (δ15N). Shaded areas correspond to periods with relatively high Chl a concentration in the upper photic layer according to ECCO-Darwin model data (see Figure 2E).
FIGURE 4. Main diatom species found by microscope examination of the sediment trap samples (<63 µm and >63 µm fractions). (A)Corethron pennatum. (B)Fragilariopsis kerguelensis.(C)Thalassiosira gracilis. (D)Chaetoceros sp. resting spores. (E)Fragilariopsis curta. (F)Fragilariopsis cylindrus).
OC and bioSi fluxes varied around averages of 1.53 mmol OC m−2d−1 and 2.86 mmol bioSi m−2d−1, respectively, and showed clear differences between months (Figure 3C and Table 2). OC represented 1–2.3% of the total mass flux, and varied from minimum OC values of 0.76 mmol OC m−2d−1 in August 2012 to maximum values of 2.38 mmol OC m−2d−1 in March 2012. bioSi fluxes were also higher in summer months, especially in December 2012, when bioSi fluxes achieved a maximum of 6.82 bioSi m−2d−1 (Figure 3C and Table 2). Furthermore, the bioSi/OC ratio that varied around a mean of 1.8 showed marked differences during the year, with a maximum of 2.95 in December 2012 (Figure 3D and Table 2). The carbon (δ13C) and nitrogen (δ15N) isotopic signal of sinking particles varied around mean values of −27.52 and 2.24, respectively; these also showed significant differences over the study period, with summer samples characterized by lower values compared to winter samples (Figure 3E and Table 2).
TABLE 2. Total mass fluxes (TMF), fluxes and concentrations of main components (OC, organic carbon; IC, inorganic carbon; bioSi, biogenic silicon) and lithogenics (litho). The C and N isotope ratios (δ13C and δ15N), and molar bioSi/OC ratio are also presented.
Relationships Between Sediment Trap Data and Modeled Environmental Variables
canonical correspondence analysis (CCA; Figure 5) evidenced the importance of both 1) upper-ocean hydrographic conditions and 2) sea-ice concentration, in determining diatom species assemblages collected by the sediment trap. The initial model CCA included: Photosynthethic Active Radiation (PAR), sea-ice concentration (sea ice), temperature, dissolved iron (dFe), stratification, chlorophyll a (chl), and particulate organic carbon (POC). POC was excluded due to VIF results, whereas PAR and Chl a were excluded on the stepwise procedure from the CCA analysis, due to non significance and low contribution to the model. The CCA final model with only four variables (stratification, temperature, sea ice, and dissolved iron content) explained 89% of the total variance in the species assemblage (adjusted R2) (Figure 5). The model was significant (F = 21.064 m p = 0.001), as well as the four environmental terms, with iron being marginally significant (F = 4.38, p = 0.06). The first two axes explained 85 and 5% respectively. Variance inflation factors (VIF) of the four terms were all below two.
FIGURE 5. RDA triplot results of the final canonical correspondence analysis (CCA) for the most relevant fossil diatom species registered in our sediment trap during the period March 2012-January 2013 (Corethron pennatum: Coreth. sp; Chaetoceros spores: Chaet. Spor.; Fragilariopsis kerguelensis: Fragil. kergu.; Thalassiosira gracilis: Tha. grac; Fragilariopsis curta: Fragil. curta; Fragilariopsis cylindrus: Fragil. cylin; Odontella weisflogii: Odont. weissf), and environmental variables (Seaice: sea ice; Strat: stratification; temp; temperature; dFe: dissolved iron). Numbers from 1 to 12 represent months from January–December. Aut: autumn (purple); Win: winter (orange); Spr: spring (green); Sum: summer (red).
The first canonical axis is primarily associated with temperature and stratification. The analysis discriminates between high/low productivity conditions, along with the species associated with each season. Month 1 (January 2013) is representative of a highly-productive period associated with Corethron pennatum. Months 6 (June 2012), 8 (August 2012), 9 (September 2012), and 10 (October 2012) correspond to periods of low productivity, associated with T. gracillis, F. cylindrus, and F. curta. The second canonical axis reflects sea-ice concentration and shows a separation of species associated with sea-ice in summer (C. pennatum) and winter (T. gracillis, F. cylindrus, and F. curta) from species less impacted by sea ice (Chaetoceros spores and Odontella weissflogii). Note also that the oceanographic variables were associated with the first canonical axis, explaining 85% of the variability in species assemblages, whereas sea ice, associated with the second axis, represents only 5% of the species assemblage variability.
Discussion
Biosiliceous organisms sinking at 1,000 m depth in the South Scotia Ridge -a naturally Fe-enriched region (Fugre 1)-, were primarily represented by diatom valves (Figure 3A). Silicoflagellates contributed only a small fraction (mean of 0.6%), and based on previous studies, radiolarians, another key contributor to biogenic silicon fluxes, appear in minor proportions in our study site (less than 1%) (Gersonde and Wefer, 1987; Abelmann and Gersonde, 1991). Our data thus corroborates that diatoms are the largest contributors of bioSi fluxes in the study area.
The fact that diatom assemblages observed at depth were primarily composed of heavily silicified species with well-preserved valves (Figure 4) highlights the role of silicification in export production, as less-silicified species may be more prone to dissolution in the upper-water column (Annett et al., 2010). We note that other diatom survival strategies such as their huge size (e.g., C. pennatum; Figure 4A) or the formation of chains (e.g., F. kerguelensis;Figure 4B) may also protect diatoms against grazing pressure (Hamm et al., 2003; Smetacek et al., 2004), and thus aiding in their ability to reach deep waters. However, the observation of small fragments during microscopic analysis also suggests the presence of less-silicified species, likely affected by dissolution during vertical export (Abelmann and Gersonde, 1991). In this regard, Nelson and Gordon (1982) estimated that, in the SO, up to 18–58% of biogenic opal might be dissolved in the upper 100 m. This implies that our bioSi content, which does not exceed 14% of the total flux (Table 2), could represent a relatively small fraction of the bioSi in the productive upper water column.
Diatom assemblage in sinking particles appear to have a major role in setting OC and bioSi export rates during our experiment year, with mean fluxes of 1.53 mmol OC m−2d−1 and 2.86 mmol bioSi m−2 d−1 (Figure 3C and Table 2)—these are in the higher range of those reported for the SO at 1000-m depth (Honjo, 2004). Strong evidence that enhanced settling of biogenic compounds occurred in close correlation with primary production in the upper water column is provided by the fact that lithogenic fluxes, as a tracer of the input of continental particles, even representing a significant fraction of the sinking material (Table 2), were not correlated with either OC nor bioSi fluxes (r2 = 0.07 and r2 = 0.05, respectively; Supplementary Figure S4). Instead, sinking OC was closely related to bioSi downward flux (r2 = 0.7; Supplementary Figure S4), suggesting that both biogenic compounds are closely linked to diatom’s production. This finding and the high proportion of well-preserved valves in the samples also suggests that the majority of diatoms recorded at depth sank from the surface, either as solitary cells or as part of fast-sinking fecal pellets and aggregates (i.e., Smetacek, 1985; Manno et al., 2015). In spite of that, OC and bioSi behave differently during their way down to the bottom. The higher bioSi/OC molar ratios in settling material (mean value of 1.8) when compared with those from ECCO-Darwin in the photic layer (average of ∼0.4) (Table 1 and Table 2), point to a preferential export of bioSi relative to OC (DeMaster, 2002; Rembauville et al., 2016). Against this background, Pilskaln et al. (2004) show that the OC exported to 1000-m depth in the SO may represent only 1% of the annual OC production in surface waters, while the preservation efficiency for bioSi is 19%. This means that deep particle fluxes obtained with sediment traps need to be carefully interpreted when attributing OC and bioSi export rates directly to exported particles and diatoms sinking.
Seasonal Succession of Diatoms Assemblage Determining bioSi/OC Variations
OC sinking fluxes down to 1000-m depth were significantly higher during austral summer periods, reflecting the end of the 2012 bloom and the early summer 2012–2013 in agreement with ECCO-Darwin Chl a concentrations (Figures 2E, 3C). The diatom assemblages during these productive periods were principally explained by two bloom-forming diatoms: Chaetoceros spp. (represented by their resting spores) and the giant C. pennatum (Figure 3B). The chain-forming, highly-silicified Fragilariopsis kerguelensis also achieved significant proportions (maximum of 25%) during those intervals. This structure of the diatom’s community corroborates that OC sequestration was characterized by species that build up high biomass under favorable growth conditions (e.g., Chaetoceros and C. pennatum) rather than species whose survival strategy is based on the maintenance of relatively constant stocks throughout the year (F. kerguelensis) (Smetacek et al., 2002; Timmermans et al., 2004; Peloquin and Smith, 2006).
Corethron pennatum fluxes seems to reflect both the end of the 2012 and the early summer 2012–13 blooms (Figures 2E, 3B). Indeed, the high correlation of C. pennatum abundances and δ13OC and δ15N isotopic signals (r2 = 0.76 and r2 = 0.77, respectively; Supplementary Figure S4) points to this species exert an important role in determining biogeochemical signature of the sinking organic matter (Figures 3B,E). This is consistent with previous findings that show a lowering δ13C (−30–−32) of settling OC when C. pennatum dominates (Bathmann et al., 1991). Moreover, our data agrees with in-situ observations at Marguerite Bay (West Antarctic Peninsula) that attribute the shift in δ13OC isotopic signals of sinking material to contrasting carbon utilization mechanisms by different diatom species (Henley et al., 2012; Shen et al., 2017).
However, we found some differences in how diatoms community structure regulate bioSi/OC molar ratio during these highly productive periods. In March 2012, despite Corethron pennatum is a relevant species, the comparatively high contribution of dense Chaetoceros spp. resting spores during this month may explain the relatively low bioSi/OC molar ratio (∼1.4) (Figures 3B,D). The reduction in this ratio due to enhanced carbon export by diatom resting spores has been observed in other Fe-rich regions of the SO (Salter et al., 2012; Rembauville et al., 2016). In contrast, during early summer 2012–2013, we found a relatively higher export of bioSi relative to OC (Figure 3D). The relatively low Chl a during December 2012, coinciding with the arrival of sea ice to our study site, suggests that in addition to the onset of the Corethron pennatum bloom (Figures 2A,E, 3B), the high bioSi export occurring during this month might be also explained by advective processes (Abelmann and Gersonde, 1991). The particular increase of the diatom species F. cylindrus, which is associated with coastal regions of Antarctica and consolidated sea ice, would also support this hypothesis (Armand et al., 2005; Lundholm and Hasle, 2008). However, the January 2013 maximum in Chl a in the photic layer, which coincide with the massive bloom of C. pennatum (Figures 2E, 3B,D) indicates that this large diatom has a significant role in favoring the export of bioSi relatively to OC to the deep ocean (bioSi/OC ratio close to two).
Environmental Factors in the Upper Photic Layer Triggering Seasonal Diatom Assemblage
Environmental conditions from ECCO-Darwin show a seasonal productivity pattern in the photic layer with a maximum of Chl a occurring during summer, in agreement with low macronutrients levels reflecting phytoplankton consumption (Figures 2E,F). Modeled Chl a and nutrient concentrations generally agree with field data previously obtained near our study site (Korb et al., 2005; Ardelan et al., 2010). The model also reproduces the consumption of dissolved Fe associated with increased summer productivity in the upper layer (Figure 2G), although the dFe background levels of ∼0.4 nM are typical of non Fe-limited regions (Dulaiova et al., 2009; DeJong et al., 2012; Measures et al., 2013). The Fe-enrichment in this study area is primarily attributed to the arrival of shelf waters from the Antarctic Peninsula (Hatta et al., 2013; Klunder et al., 2014). Additionally, local sea-ice melt -as occurred in January 2013-, is another known source of dissolved Fe in this region (Wang et al., 2014; Lannuzel and Chever, 2016; Monien et al., 2017).
Sinking diatom assemblages, which follow the seasonal trend of environmental variables in the upper photic layer was reflected in the ordination technique canonical correspondence analysis, where we assume that sinking rates are high enough for the particles to sink to 1,000 m depth in less than 30 days (Figure 5). This assumption has been considered in previous SO studies (e.g., Pilskaln et al., 2004; Fisher and Karakaç, 2009; Rigual-Hernandez et al., 2019). Considering this, our analysis shows that, apart from irradiance and dFe, other environmental factors such as water column stratification of the water column need to be considered as triggers of phytoplankton blooms. This means that increased stratification, whether it occurs at the end of summer due to heating of the surface layer (March-April 2012), or it is associated with sea ice melt, as occurred in early summer 2012–2013, plays a key role in promoting C. pennatum blooms (Figures 2D, 3B, 5). Such massive blooms have been previously observed close to our study site (Gersonde and (Wefer, 1987; Fryxell, 1989) as well as in the vicinity of South Georgia Island (Froneman et al., 1995, 1997), and at frontal zones in the Atlantic sector of the SO (Laubscher et al., 1993; Bathmann et al., 1997). Our data suggests that sea ice may trigger an early summer bloom, as recently observed in the Arctic Ocean (Boetius et al., 2013; Clement-Kinney et al., 2020). This may occur via two main processes. First, local melting of sea ice can result in an additional flux of dissolved nutrients (such as Fe) to near-surface waters (Lannuzel and Chever, 2016). This might provide the extra nutrient supply needed to promote blooms and the high ambient Fe concentrations required by the large, slow growing C. pennatum to reach optimal growth rates (Timmermans et al., 2004; Smetacek et al., 2004; Hoffmann et al., 2006). Second, the capacity of C. pennatum to adjust its buoyancy would provide an advantage for exploiting nutrients in stratified waters, allowing for blooms under low-light conditions (as reproduced by ECCO-Darwin; Figure 2B). Though C. pennatum buoyancy adjustment has only been reported by Crawford (1995), this mechanism was observed for other large diatoms (e.g. Rhizosolenia and Proboscia) (Villareal et al., 1993, 1999a, 1999b; Moore and Villareal, 1996; Singler and Villareal, 2005; Kemp et al., 2006). This supports the idea that Corethron might also be adapted to exploit a stratified water column (via sea ice melt) and deep nutrient sources. In this context, Chl a maxima associated with sea-ice melt was attributed to C. pennatum in the Atlantic sector of the SO (Fryxell, 1989), and in the South Georgia region (Whitehouse et al., 2008; Nunes et al., 2019). The blooming of this large diatom, combined with its morphological characteristics (such as the presence of a set of shorted barbed spines that favor entanglement and aggregation, or its large size that allow scape grazing, probably favor larger export into the deep ocean (Smetacek, 1985; Alldredge and Gotschalk, 1989; Smetacek et al., 2004). Increased sinking of C. pennatum half-cell walls may occur due to the fall-down of a sexual reproductive phase event (Crawford, 1995), but the absence of half-cells in the samples prevent us from confirming this hypothesis. Accordingly, this data supports the assumption used by paleoceanographers where C. pennatum creates and rapidly exports substantial biomass under stratified conditions during times of enhanced sea-ice melt (Jordan et al., 1991; Leventer et al., 1993; Sedwick et al., 2001; Leventer et al., 2002; Taylor and Sjunneskog, 2002; Maddison et al., 2012; Alley et al., 2018).
The role of stratification in promoting C. pennatum blooms is also supported by the observed changes in the sinking organic matter total nitrogen (TN) and OC isotopic composition, which are well-established proxies for assimilation of surface-ocean nitrate and dissolved inorganic carbon (DIC) by phytoplankton (Sigman et al., 1999). Exported organic matter shows relatively low δ15N values (1.2–1.6‰) in periods when C. pennatum dominates the diatoms assemblage (Figures 3B,E). These values are significantly lower than the typical summer δ15N values of surface-ocean nitrate (>5‰) (Sigman et al., 2000), suggesting a shift from high δ15N -NO3 to low δ15N -NH4+ as the primary nitrogen source exploitable by these large blooming diatoms. However, this does not agree with the assumption that NH4+-assimilating phytoplankton are typically smaller in size (Berg et al., 2011). Another possibility is that phytoplankton utilize under-ice NH4+ and DIC with low δ13C (because of low ventilation). However, low δ15N and δ13OC were also recorded during sea-ice free conditions in February 2012. Yet, the robust positive correlation of δ13OC and δ15N (r2 = 0.74; Supplementary Figure S4) suggests that the mechanism responsible for low δ15N is also decreasing the δ13OC of sinking particles. If assimilation of low 13OC DIC relatively to ambient DIC occurs deeper in the water column, then vertical migration due to buoyancy regulation of C. pennatum would also explain the use of lighter 14N from the nutricline and near-surface waters, triggering lower δ15N in settling particles.
Conclusion
Settling material collected by a sediment trap at 1000 m depth in the South Scotia Ridge provides, for the first time, an almost complete annual cycle of diatom abundance and composition in the southern sector of the Scotia Sea. A statistical analysis of in-situ data and realistic ocean biogeochemistry simulation shows that the material collected by the sediment trap reflects changes in upper-ocean environmental conditions. Additionally, sediment trap data provide geochemical evidence that massive C. pennatum blooms occuring in highly-stratified waters thrive during early summer sea-ice melt conditions. Consequently, the sedimentation of these large diatoms enhance silicon removal from SO waters. Our results, together with similar studies that report high bioSi/OC ratios in other Fe-rich SO regions, challenge the conventional view of diatoms growing under Fe-replete conditions as drivers of sinking high OC to bioSi fluxes. We conclude that, along with irradiance and dFe, sea ice concentration (which modulates changes in upper-ocean stratification), needs to be considered when determining which environmental factors trigger specific diatoms blooms, that, in turn, determine carbon sequestration. To our knowledge, this is a novel aspect of diatoms ecology in setting bioSi vs. OC sequestration efficiency—a key controlling factor that regulates the stoichiometric relationship of limiting nutrients for primary production. Ultimately, additional studies that combine water column environmental conditions and surface-to-bottom sediment trap data are required to improve our understanding of diatom dynamics and the coupled physical-biogeochemical processes that regulate export in the Southern Ocean.
Data Availability Statement
The datasets presented in this study can be found in online repositories. The names of the repository/repositories and accession number(s) can be found below: The datasets analyzed for this study have been deposited at the Spanish National Polar Data Center (CNDP), http://hielo.igme.es/index.php/en/. ECCO-Darwin model fields are available at: https://data.nas.nasa.gov/ecco.
Author Contributions
DZ, AS-V and MMF contributed equally to the writing of the manuscript. MMF conceived, designed the monitoring experiment and acquired the data. AS-V. performed biogeochemical analyses and acquired the data. DZ counted and identified diatom assemblage. DC provided ECCO-Darwin time series and helped with manuscript editing and figure creation. MR performed the statistical analysis. FA provided relevant information for diatoms identification and contributed to the writing of the manuscript. GS contributed with sea-ice analysis and prepared Supplementary Figures S1–S3. TC contributed to the writting of the manuscript and provide valuable support during the whole process. All authors read, edited, and approved the final version of the manuscript.
Funding
This work was funded by the Spanish Polar Program through the Spanish Research and Innovation (I+D+i) National Plan (grant numbers CTM2009-08287-E/ANT and CTM2011-14056- E/ANT), and supported by the Catalan Government Grups de Recerca Consolidats Grant (2017 SGR 315) and the Internal Research and Technology Development program of the Jet Propulsion Laboratory, California Institute of Technology. DZ was funded by a postdoctoral fellowship (Plan I2C) from Xunta de Galicia (Spain) and performed diatom analysis during her stay at Instituto Português do Mar e da Atmosfera (IPMA), Lisbon, Portugal. Diatom analysis was sponsored by Portuguese national funding through FCT-Fundação para a Ciência e a Tecnologia (UIDB/04326/2020 and DiatBIo PTDC/AAG-GLO/3737/2012 projects). GS was supported by the Deutsche Forschungsgemeinschaft (DFG) in the framework of the priority programme “Antarctic Research with comparative investigations in Arctic ice areas” SPP 1158 by Grant SITAnt (365778379).
Conflict of Interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Acknowledgments
The authors are deeply grateful to Joan Puigdefàbregas and Jordi Cateura for their technical assistance in mooring deployment and recovery; Rut Pedrosa-Pàmies and Montse Guart for their help with analytical tasks; the Captain and crew of the R/V Hespérides for their support during the 2012 and 2013 Antarctic cruises.
Supplementary Material
The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2021.579198/full#supplementary-material
Supplementary Figure 1 | Sea ice velocity fields for the months of November 2012, December 2012 and January 2013 obtained from the NASA National Snow and Ice Data Center Distributed Active Archive Center (Tschudi et al., 2016). Sea ice was strongly advected into the study area during November and December, and the advection stopped in January.
Supplementary Figure 2 | December 2012 sea ice concentration anomaly relative to the reference period 1979–2016. Antarctic Circumpolar Current fronts, after Orsi et al. (1995), are indicated as dashed contours (names labeled). The sediment trap location (60° 24’S; 52° 58’W) is marked by a black star. Gray lines mark parallels and meridians.
Supplementary Figure 3 | Sea ice persistence for the month of December during the 1979–2016 period. Sea-ice persistence gives the frequency of sea ice occurrence (how often sea ice is present) at a given location. Sea ice persistence of 100% means that the area was always covered by sea ice throughout December within the 38-year period 1979–2016; 0% means the opposite: no sea ice was ever present. The mooring location is marked with a star. Sea ice persistence at the mooring location is 2% or 24 days, i.e., 2012 was the only year in which sea ice was observed at that location during the month of December.
Supplementary Figure 4 | Pearson correlation matrix for the sediment trap data. Lithog flux: lithogenic flux (mmol m−2 d−1), OC: organic carbon flux (mmol m−2 d−1) and relative contribution (%), bioSi: biogenic silicon flux (mmol m−2 d−1) and relative contribution (%), biogeochemical variables (d13C= organic carbon isotope ratio; d15N= total nitrogen isotope ratio; bioSi/OC: biogenic silicon/organic carbon molar ratio), and most representative fossil diatoms species (Corethron pennatum: Coreth. sp; Chaetoceros spores: Chaet.Spor.; Fragilariopsis kerguelensis: Fragil.kergu.; Thalassiosira gracilis: Thal.grac; Fragilariopsis curta: Fragil. curta; Fragilariopsis cylindrus: Fragil. cylin; Odontella weisflogii: Odont.weissf) abundances expressed in valves m−2 d−1).
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Keywords: diatoms, sea ice, marginal ice zone, carbon export, biogenic silicon, scotia sea, southern ocean, corethron pennatum
Citation: Zúñiga D, Sanchez-Vidal A, Flexas MM, Carroll D, Rufino MM, Spreen G, Calafat A and Abrantes F (2021) Sinking Diatom Assemblages as a Key Driver for Deep Carbon and Silicon Export in the Scotia Sea (Southern Ocean). Front. Earth Sci. 9:579198. doi: 10.3389/feart.2021.579198
Received: 01 July 2020; Accepted: 26 May 2021;
Published: 17 June 2021.
Edited by:
Maureen H Conte, Bermuda Institute of Ocean Sciences, BermudaReviewed by:
Ian Salter, Alfred Wegener Institute Helmholtz Centre for Polar and Marine Research (AWI), GermanyTom Trull, Commonwealth Scientific and Industrial Research Organisation (CSIRO), Australia
Copyright © 2021 Zúñiga, Sanchez-Vidal, Flexas, Carroll, Rufino, Spreen, Calafat and Abrantes. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: D. Zúñiga, aW1pc3NvbnNAZ21haWwuY29t