Climate change at the Western Antarctic Peninsula (WAP) is predicted to cause major changes in phytoplankton community composition, however, detailed seasonal field data remain limited and it is largely unknown how (changes in) environmental factors influence cell size and ecosystem function. Physicochemical drivers of phytoplankton community abundance, taxonomic composition and size class were studied over two productive austral seasons in the coastal waters of the climatically sensitive WAP. Ice type (fast, grease, pack or brash ice) was important in structuring the pre-bloom phytoplankton community as well as cell size of the summer phytoplankton bloom. Maximum biomass accumulation was regulated by light and nutrient availability, which in turn were regulated by wind-driven mixing events. The proportion of larger-sized (> 20 µm) diatoms increased under prolonged summer stratification in combination with frequent and moderate-strength wind-induced mixing. Canonical correspondence analysis showed that relatively high temperature was correlated with nano-sized cryptophytes, whereas prymnesiophytes (Phaeocystis antarctica) increased in association with high irradiance and low salinities. During autumn of Season 1, a large bloom of 4.5-µm-sized diatoms occurred under conditions of seawater temperature > 0 °C and relatively high light and phosphate concentrations. This bloom was followed by a succession of larger nano-sized diatoms (11.4 µm) related to reductions in phosphate and light availability. Our results demonstrate that flow cytometry in combination with chemotaxonomy and size fractionation provides a powerful approach to monitor phytoplankton community dynamics in the rapidly warming Antarctic coastal waters.
Global climate change will have consequences for marine ecosystems throughout the world’s oceans (Boyce et al. 2010; Hallegraeff 2010). In polar marine ecosystems, the impact of a warming climate is magnified because a relatively small change in temperature can have a large impact on sea ice melt and ice cover (Smetacek and Nicol 2005; Schofield et al. 2010). In the Antarctic, declines in sea ice have been associated with a longer growing season and consequently, higher annual net production (Moreau et al. 2015). However, the influence of sea ice is complicated by variability in relation to the extent as well as the timing of advance and retreat which may be largely influenced by local-scale, rather than large-scale, forcing (Kim et al. 2018). Decreased ice cover has been associated with a reduction in photosynthetic efficiency (Schofield et al. 2018) and several studies have described a reduction in overall phytoplankton biomass and a shift from large phytoplankton (diatoms) to smaller flagellated species. These shifts have been associated with reduced salinities, higher temperatures and stronger vertical stratification (Moline and Prezelin 1996; Moline et al. 2004; Montes-Hugo et al. 2009; Venables et al. 2013; Mendes et al. 2017; Rozema et al. 2017c). However, the physicochemical drivers behind community shifts towards flagellated phytoplankton remain unclear, likely due to the diversity among flagellated phytoplankton spanning different taxonomic groups and cell sizes, and each may interact differently with the physicochemical environment. Our current understanding of the drivers associated with the seasonal progression within the phytoplankton community (Henley et al. 2019), particularly the pico- (≤ 3 µm) and nano-sized (> 3–20 µm) phytoplankton, limits our ability to accurately predict how polar marine systems will respond to future climate change with implications for food-web dynamics and the marine carbon cycle (e.g. Pinhassi et al. 2004; Conan et al. 2007; Christaki et al. 2008; Obernosterer et al. 2008; Agustí and Duarte 2013; Evans et al. 2017).
Cell size is an important functional trait that influences almost every aspect of phytoplankton biology (Marañón 2015). Phytoplankton community size structure is therefore a key factor regulating food-web dynamics, biogeochemical cycling and trophic carbon transfer in the marine environment (Finkel et al. 2010; Marañón 2015). Shifts in the size class of primary producers in productive regions may also affect ocean carbon sequestration (the biological pump) as the larger phytoplankton (e.g. diatoms) are typically grazed by large copepods and krill (Quetin and Ross 1985; Jacques and Panouse 1991; Kopczynska 1992; Granĺi et al. 1993), whereas the smaller-sized cells (flagellates) are grazed by salps, small copepods and protozoans (Harbison et al. 1986; Riegman et al. 1993; Froneman and Perissinotto 1996; Perissinotto and Pakhomov 1998). As a result, obtaining a mechanistic understanding of the factors that control the variability of phytoplankton community size structure remains a central goal in biological oceanography (Marañón 2015).
The Western Antarctic Peninsula (WAP) has experienced rapid climate change (Saba et al. 2014) resulting in alterations in phytoplankton community structure (Beardall and Stojkovic 2006; Deppeler and Davidson 2017; Rozema et al. 2017c), which are evident at higher trophic levels, with shifts in the grazer community from krill to the nutritionally poorer salps (Loeb et al. 1997; Atkinson et al. 2004; Saba et al. 2014; Steinberg et al. 2015). Moreover, reduced viral activity predicted due to changes in host population dynamics (Evans et al. 2017), may exacerbate impacts on community structure due to reduced substrate availability for microbial loop processes. Although the WAP area has been studied in quite some detail over the last 20 years, to our knowledge, no studies have simultaneously investigated the size class distribution of Antarctic phytoplankton abundances using flow cytometry (FCM) and chemotaxonomy (CHEMTAX). Thus far, WAP phytoplankton communities have been examined using mostly light microscopy and/or pigment-based taxonomic analysis (Garibotti et al. 2003, 2005; Rozema et al. 2017c). Studies using flow cytometry (FCM) to investigate phytoplankton community composition and examine environmental drivers are still lacking. Furthermore, fractionated Chlorophyll-a (Chl-a) studies did not include taxonomic distinction of the different size classes and investigated long-term trends and inter-seasonal differences rather than intra-seasonal variation (Clarke et al. 2008; Rozema et al. 2017c). Here we describe phytoplankton community dynamics (abundances, taxonomic composition and size of single cells) over two consecutive productive seasons. The combination of FCM and CHEMTAX, with size fractionation, potentially represents a powerful approach to uncover physicochemical factors structuring phytoplankton community size structure, particularly the pico- and nano-sized classes.
Study area and sampling
Data for this study were obtained at the Rothera time series site (RaTS, latitude 67.572°S; longitude 68.231°W; Clarke et al. 2008) located in Ryder Bay on the WAP (Fig. 1). Samples were taken over two consecutive austral productive seasons designated S1 (November 2012 to April 2013) and S2 (November 2013 to April 2014). Discrete seawater samples were collected from 15 m depth by a 12-L Niskin bottle deployed from a small boat. Full water column profiles were obtained using a SeaBird 19 + conductivity temperature depth instrument (CTD) supplemented with a flat LiCor sensor to measure photosynthetically available radiation (PAR) and an in-line fluorescence sensor (WetLabs). Calibration of the CTDs between years is discussed in Venables et al. (2013). Sampling for physicochemical variables, FCM abundances and phytoplankton pigments was conducted approximately twice weekly. Water samples were shielded from the light and processed as soon as possible in a temperature-controlled lab maintained at c.a. 0.5–1 °C.
Density, temperature, salinity and PAR were obtained from the CTD. Sampling was conducted when the study site was ice free and accessible by boat (i.e. no CTD casts were performed under sea ice). Euphotic zone depth (Zeu) was calculated as the depth at which PAR was 1% of surface (1 m) PAR. As an index to determine possible light limitation at the sampling depth, Zeu was divided by 15 m (Zeu/15 m), whereby a score < 1 indicates possible light limitation (phytoplankton are below the euphotic zone) and > 1 no (or reducing probability of) light limitation. Stratification was quantified as the potential energy required to homogenize the water column from the surface to 40 m depth (J m−2) according to Venables et al. (2013). MLD was defined as a 0.05 kg m−3 difference in density relative to the surface (Venables et al. 2013). Sea ice type and coverage (%) was determined routinely every day in Ryder Bay by visual observation by Rothera base staff, with the Rothera records agreeing well with wider scale satellite-derived trends (see Venables et al. 2013). Definitions for ice type (as defined by the British Antarctic Survey) were as follows: fast ice is a solid sheet of ice attached to the land, pack ice is a large area of sea ice that is not land fast, brash ice is small fragments of floating ice, grease ice is a very thin layer of frazil ice (ice crystals formed in water that is too turbulent to freeze solid) and pancake ice is round pieces of newly formed ice (from grease ice). Discrete water samples (6 mL) for dissolved inorganic phosphate, nitrate, nitrite, and silicate, were gently filtered through 0.2-µm pore-size Supor membrane Acrodisk filters (25 mm diameter, Pall, Port Washington, NY 11050, USA). Ammonium samples were collected and analysed as in Clarke et al. (2008). Silicate samples were stored at 4 °C and those for nitrogen and phosphorus at − 20 °C until further analysis according to procedures described in detail by Bown et al. (2017).
For phytoplankton enumeration (of single cells), fixed samples were counted during S1 and fresh (live) samples during S2. Technical problems with the flow cytometer during S1 prohibited live counts of phytoplankton abundances. No significant difference was found in phytoplankton population counts between live and fixed samples (Mann–Whitney Rank Sum Test: p = 0.24, n = 44). For S1, 3.5 mL subsamples were fixed with 100 µL formaldehyde–hexamine (18% v/v:10% w/v) at 4 °C for 15–30 min, after which they were snap-frozen in liquid nitrogen and stored at − 80 °C until analysis. Samples were analysed according to Marie et al. (1999) using a Becton–Dickinson FACSCalibur FCM equipped with an air-cooled Argon laser with an excitation wavelength of 488 nm (15 mW) and the trigger was set on red fluorescence. Phytoplankton populations were distinguished using bivariate scatter plots of red Chlorophyll-a (Chl-a) autofluorescence versus side scatter. Cryptophytes were discriminated based on their orange phycoerythrin autofluorescence. The FCM data files were analysed using the freeware CYTOWIN (Vaulot 1989). No indications of chains or colonies were found in FCM cytograms.
During the summer months, approximately weekly size fractionations were performed to determine the average cell size of the different phytoplankton populations distinguished using FCM. A whole water sample (5–10 mL) was gently filtered through either a 50-, 20-, 10-, 8-, 5-, 3-, 2-, 1-, 0.65-, or 0.4-µm pore-size filters. The filtrates were then analysed by FCM as described previously. Mean cell size was calculated as the size corresponding to a 50% retention of cells based on the fit of an S-shaped plot (i.e. number of cells retained versus the pore size; Veldhuis and Kraay 2004). Over the course of both seasons, a total of 10 phytoplankton populations were distinguished, referred to as Phyto I to Phyto X according to increasing average cell diameter (Table 1).
Vertical profiles (published in Bown et al. 2017; Rozema et al. 2017b) indicate that fluorescence-based Chl-a concentrations at 15 m were most often comparable to subsurface Chlorophyll maximum (SCM). For Chl-a concentration and taxonomic composition, 1-8 L of whole seawater was filtered over GF/F glass fibre filters (47 mm, Whatman, The Netherlands). Filters were wrapped in aluminium foil, snap-frozen in liquid nitrogen and stored at -80 °C until analysis. For the majority of samples, phytoplankton pigments were analysed by high performance liquid chromatography (HPLC) according to Brussaard et al. (2016). Three phytoplankton samples in S1 and 8 phytoplankton samples in S2 were analysed by HPLC according to Rozema et al. (2017a), as these samples were part of the BAS monitoring project. The pigment concentrations extracted and detected by the two separate approaches were not significantly different (p < 0.0001; R2 = 0.99, n = 39) for natural samples collected in situ (Online Resource 1). In both cases, pigment quantification was performed using standards (DHI, Hørsholm, Denmark) for Chlorophyll c3, Peridinin, 19′-Butanoyloxyfucoxanthin, Fucoxanthin, Neoxanthin, 19′-Hexa-fucoxanthin, Alloxanthin, Lutein, Chlorophyll b, Chl-a, and identified peaks were manually checked for quality assessment. Phytoplankton class abundances were calculated using pigment data from HPLC by CHEMTAX v1.95 (Mackey et al. 1996). This programme uses a factor analysis and the steepest decent algorithm to find the best fit based on a pigment ratio matrix. Six different taxonomic phytoplankton classes were chosen to represent the WAP marine ecosystem, identical to those used previously for the RaTS time series (Rozema et al. 2017a) and confirmed by microscopy observations (unpublished data): Prasinophyceae, Chlorophyceae, Dinophyceae, Cryptophyceae, Prymnesiophyceae and Bacillariophyceae (diatoms). Unfractionated pigment concentration data were sorted into two bins depending on season (S1 and S2). Additionally, size-fractionated samples were also binned per season. CHEMTAX was run 60 times per bin with randomized (± 35%) pigment ratios to minimize the root mean square error (RMSE) using settings recommended in Kozlowski et al. (2011). The run with the lowest RMSE was deemed final with initial and final ratios shown in Online Resource 2.
Within each season (S1 and S2), four distinct periods were identified based on the temporal dynamics of Chl-a concentration: no bloom (NB) from 1 to 29 November, and bloom 1–3 (B1–3) from 30 November to 8/9 January, 9/10 January to 10/14 February, and 11/15 February to 15 April, respectively.
In general size fractionation of whole water for pigment analysis was performed once a week during the summer months. Between 1 and 5 L of whole seawater was pre-sieved through different filters (20 and 5 µm) and then filtered over a 47-mm GF/F glass fibre filter (Whatman, 0.7 µm nominal pore size) to obtain size fractions > 20, 5–20 and < 5 µm. Filters were subsequently snap-frozen in liquid nitrogen wrapped in aluminium foil and stored at − 80 °C until analysis.
To allow for a better comparison between FCM and CHEMTAX data, phytoplankton abundances and taxon-specific Chl-a concentrations were converted to cellular carbon (C). The C content of each phytoplankton population identified by FCM (FCM-C) was estimated from the average cell diameter (assuming cells to be spherical) using conversion factors of 196.5 and 237 fg C µm−3 for nano- and pico-sized phytoplankton populations, respectively (Garrison et al. 2000; Worden et al. 2004). Carbon conversion factors may vary, depending on taxonomy, cell size and growth-regulating factors such as light and nutrient availability (Geider 1987; Álvarez et al. 2017). Cell size variation was taken into account by using size-dependent conversion factors for the various FCM phytoplankton clusters (Phyto I-X). To accommodate for taxonomic variations in cellular Chl-a concentrations (Geider 1987; Álvarez et al. 2017), we used different conversion factors (also reflecting cell size) for the classified groups (e.g. diatoms and cryptophytes). Carbon estimates for the different phytoplankton taxonomic groups were thus obtained from taxon-specific Chl-a concentration multiplied by taxon-specific conversion factors according to Garibotti et al. (2003), with the exception of Dinophyceae for which an average of ratios by Llewellyn et al. (2005) and Agirbas et al. (2015) were used. Moreover, for the dominating diatoms and cryptophytes, it was possible to refine carbon estimates based on Chl-a (named Chl-C) using published conversion factors specific for different biomass concentrations (according to Garibotti et al. 2003), i.e. low < 1, medium 1–4 and high > 4 µg Chl-a L−1 dominated by small-, nano- and micro-sized phytoplankton, respectively. The only exception was during B3 of S1, where the medium biomass C:Chl-a ratio was used due to the dominance of total Chl-a by nano-sized phytoplankton (Online Resource 4) despite high Chl-a concentrations. For the majority of both seasons, Chl-a cell−1 (≤ 20 µm) ranged between 0.1 and 0.8 pg.
The C to Chl-a ratios used in this study originate from Garibotti et al. (2003; with reference to Montagnes and Franklin 2001 and Montagnes et al. 1994) who used different taxonomic groups and cell sizes with culture light conditions below light saturation (50 µmol photons m−2 s−1), more representative of natural conditions. However, it is difficult to correct for potential seasonal variability of (natural variation in) carbon conversion factors (not already covered by us). Chl-a (< 20 µm) varied between 0.1 and 4.1 pg cell−1 and was within range of experimental values (Álvarez et al. 2017). Cellular Chl-a content was only higher (i.e. > 0.8 pg cell−1) during the B3 bloom of S1 when PAR reduced to very low levels, indicating possible photoacclimation. However, increased Chl-a cell−1 was most likely the result of a change in community composition as larger cells (from Phyto VI to Phyto IX) increasingly dominated Chl-a (< 20 µm). Furthermore, size fractionation on 13th March indicated that the average diameter of Phyto IX had also increased from 11 to 12–15 µm.
To check for potential differences in FCM abundances between fresh and fixed phytoplankton samples, a Mann–Whitney Rank Sum Test (SigmaPlot 14.0) was performed on 44 population counts from 8 samples spread over S2.
Canonical correspondence analysis (CCA) was performed on measured data using the R statistical software (R Development Core Team 2012) supplemented with Vegan (Oksanen et al. 2013). Data exploration was carried out according to the protocol described in Zuur et al. (2010). A combined forward–backward selection procedure was applied to select only those explanatory variables that contributed significantly to the CCA model, while removing non-significant terms. Significance was assessed by a permutation test, using the multivariate pseudo-F value as the test statistic (Zuur et al. 2009). A total of 999 permutations were used to estimate p values associated with the Pseudo-F statistic. To identify and remove any collinearity from final models, variance inflation factors (VIF) were calculated. Sequentially, explanatory variables with the largest VIF were removed until all variables resulting in VIF < 10 (Zuur et al. 2009). The environmental variables (after VIF selection) included as constraining variables in the multivariate analysis were temperature, salinity, PAR, MLD, Zeu/15 m, stratification (Strat), phosphate, nitrate, silicate, wind speed and ice cover. Additionally, ice type (levels) and seasons (S1 and S2) were added as factors to see how they relate to phytoplankton abundance and taxonomic composition. PAR, MLD, Zeu/15 m, phosphate and nitrate data were log transformed due to their non-linear relationship to total biomass, and to reduce the effects of outliers. CTD casts were absent for 13 phytoplankton abundance samples and 17 pigment samples from S1, and 9 from both sample types of S2. To overcome this limitation and permit data to be included into the CCA, the time series data (temperature, salinity, PAR, MLD, Zeu/15 m and Strat) were linearly interpolated. For most of those samples (80%), CTD casts were taken within 1 day (and often 1 day before and 1 day after) of biological samples and the remaining were taken within 2 days (apart from 1 sample taken 3 days apart). Five data points (spread evenly over the season) in S1 and 1 data point in S2 were missing nutrient data, and so interpolated data were also used for these 6 time points.
The analysis of biological variables consisted of phytoplankton abundance (FCM) and carbon biomass (converted from FCM), and pigment-based phytoplankton taxonomic community composition (in Chl-a) and taxon-specific carbon biomass (converted from Chl-a). Note that for Chl-a data, ‘season’ did not contribute significantly to the model, allowing for combined analysis of both seasons. For FCM data, season was a significant factor and subsequently S1 and S2 data sets were ran separately.
When interpreting CCA correlation triplots, arrow lengths represent the covariates and their correlation with the axes (CCA1 horizontal axis and CCA2 vertical axis). The correlation between response variables is reflected in the angles between lines, wherein, a small angle between two lines represents a high positive correlation, a 90° angle represents no correlation and 180o a strong negative correlation.
At the beginning of November in S1, Ryder Bay was completely covered by fast ice which rapidly declined to 10% by mid-December (Fig. 2a). For the remainder of S1, brash ice was the main ice type with gradual declining cover (from 80 to 10%) until mid-January after which it remained relatively low but with considerable variability. At the beginning of S2, grease ice was the dominated ice type (up to 100% cover), but ice cover rapidly changed to pack ice and declined in extent to 10% by 17th November. Following this, brash ice took over and cover increased to 100% (Fig. 2b). A short period of pack ice cover was observed in mid-December, returning into brash ice as ice cover rapidly declined during the second half of December. For the remainder of the season, brash ice remained generally low but variable (10–80%).
Stratification increased steadily at the beginning of December in both seasons (Fig. 2c) accompanied by a shallowing of the MLD (Fig. 2d). Stratification peaked at the end of December (1544 in S1 and 1264 J m−2 in S2) and then declined during the first half of January in both seasons. In S2, stratification increased again and remained high until 10th February. This difference in stratification between the two seasons was apparent in MLD which was deeper in S1 at 16 ± 8 m (n = 3) compared to 2 ± 1 m (n = 3) during the same period of S2. Stratification levels were weak for both seasons in March and April, and MLD were relatively high ranging from 20 to 40 m.
In both seasons, seawater temperature steadily increased from − 1.7 °C in November to 0 °C during early January (Fig. 3a). Temperature during S1 peaked at 1.9 °C on 16th January and remained around 1.2 °C for 1 month before gradually declining to below 0 °C in April. In S2, seawater temperature peaked later in the season (1.4 °C on 5th February) and declined to < 0 °C in early February, followed by a gradual decrease to around − 1.1 °C in April. Compared to S1, average temperature during S2 was ~ 2.5-fold lower (0.36 ± 1 vs. − 0.45 ± 0.6 °C, n = 39 and 50, respectively), with the strongest difference during bloom period B2 (1.09 ± 0.62 vs. 0.09 ± 0.63 °C, n = 13 and 16, respectively) and B3 (half February to April; 0.64 ± 0.49 vs. − 0.55 ± 0.40 °C, n = 15 and 11, respectively). Salinity gradually declined until January during S1 (Fig. 3b), whereas in S2, a rapid drop was observed during January, and values remained low for 3 weeks before stabilising at ~ 33.0 psu by March, slightly lower than the salinity of 33.2 psu in S1 over this period. PAR levels were the highest at the start of both seasons (Fig. 3c), declining thereafter to potentially growth-limiting levels (as indicated by Zeu/15 m; Fig. 3d) and reaching values as low as 0.3–0.4 µmol quanta m−2 s−1 by the second half of December. During the B2 bloom period of S2, PAR was generally low (17 ± 23 µmol quanta m−2 s−1, n = 15) and had a higher potential for light limitation compared to the same period in S1. Conversely, during the bloom period B3 of S1, PAR levels (< 3 µmol quanta m−2 s−1) were much lower compared to S2.
Phosphate and nitrate in S1 were drawn down from concentrations of 1.7 and 28 µM on 8th Dec to 0.17 and 1.3 µM, respectively, at the start of January, before rising again until mid-February (Online Resource 3). In S2, the initial drawdowns of phosphate and nitrate were more gradual and variable than S1, lasting until the beginning of February and reaching 0.04 and 0.03 µM, respectively. A second large drawdown of phosphate was observed during S1, declining to 0.06 µM on 12th March. Ammonium concentrations were initially low in both seasons (~ 0.35 µM) and increased to 5 µM on 5th February in S1 and 2.6 µM on 17th February in S2 (Online Resource 3). Silicate concentrations remained replete over the observation period of both seasons (Online Resource 3), as were concentrations of dissolved iron (DFe, Bown et al. 2017).
Chlorophyll-a and taxonomic groups
The mean Chl-a concentration in S1 (4.3 ± 4.4 µg L−1, n = 51) was 1.6-fold higher than in S2 (2.7 ± 2.2 µg L−1, n = 50, Fig. 4). This was due to the S1 phytoplankton blooms (i.e. peaks in Chl-a) during bloom periods B1 and B3 (12.3 and 16.1 µg Chl-a L−1, respectively). In contrast, the B2 period in S2 displayed a higher mean Chl-a concentration than that in S1, i.e. 4.6 ± 1.7 and 2.0 ± 1.5 µg L−1, n = 17 and 16, respectively. Diatoms (Bacillariophyceae) often dominated total Chl-a both during S1 and S2 (Fig. 4c, d), but at the start of S2 (NB period), Prymnesiophyceae and Prasinophyceae both dominated, and during B2 in S1, Cryptophyceae contributed most to total Chl-a concentration. Furthermore, at the start of B3 (second half of February) for both S1 and S2 the Cryptophyceae and Prymnesiophyceae co-dominated, while towards the end of B3 in S2, Prasinophyceae were most important. Contributions to Chl-a by Chlorophyceae and Dinophyceae were marginal over both seasons of this study.
Size-fractionated Chl-a shows that initially during the NB period when total Chl-a concentrations were still low (Fig. 4), the phytoplankton community was mostly < 20 µm (Online Resource 4). Temporal Chl-a size fraction dynamics in S1 revealed a shift from larger-sized (> 20 µm) phytoplankton during the first bloom period B1 to smaller-sized phytoplankton during the remainder of the season (up to 89% of total Chl-a in B3; Online Resource 4a). In contrast, relatively smaller (< 20 µm) cells contributed most to phytoplankton biomass during the initial increase during B1 in S2 and larger cells dominating during B2 (Online Resource 4b). Taxonomic analysis of fractionated Chl-a revealed that diatoms and Cryptophyceae were present in all the three size fractions. Prymnesiophyceae were present largely in the < 5 µm fraction but were also observed in the > 20 µm fraction, during March (B3) in S1 and late January to beginning of February in S2, presumably indicative for P. antarctica colonies (confirmed by light microscopy, data not shown).
Canonical correspondence analysis (CCA) was used to investigate the relationship between taxonomic composition (in Chl-a concentration) and the environmental variables with both S1 and S2 combined. The eigenvalues (obtained from the model output; Online Resource 5) indicated that the main environmental variables contributing to the formation of the axes explained 35% of total variation in the dataset (23 and 11% for first and second axes, respectively). These variables were temperature (p < 0.001, n = 101), Zeu/15 m (p < 0.001, n = 101), salinity (p = 0.058, n = 101), phosphate (p = 0.005, n = 101) and nitrate (p = 0.039, n = 101, Fig. 5a). Overall, higher concentrations of Cryptophyceae were associated with high temperature (> 1 °C) and Prymnesiophyceae with relatively high Zeu/15 m and low salinity. More specifically, the B2 data points in S1 clustered with high temperature and Cryptophyceae Chl-a, which were both highest during this period.
Phytoplankton abundance (and taxonomy)
The 10 phytoplankton clusters distinguished by FCM (Fig. 6) could be partially characterized (taxonomically). Temporal dynamics of Phyto III matched well with the dynamics of Prymnesiophyceae and light microscopy confirmed co-occurrence of P. antarctica single cells at times of high Phyto III abundances. Phyto III cell size (range 2–5 µm in diameter) corresponds to that of solitary P. antarctica cells (between 2 and 6 µm, Schoemann et al. 2005; Lee et al. 2016). Phyto IV dynamics compared well to Cryptophyceae Chl-a (< 20 µm, Online Resource 6) and was identified as a cryptophyte group based on high orange (phycoerythrin) autofluorescence (Li and Dickie 2001) in combination with microscopic identification during times of high abundance. Phyto V-X are most likely diatoms, based on the good comparison of relative carbon contribution of individual phytoplankton groups with CHEMTAX analysis of specific Chl-a size fractions (at times when large group-specific carbon contributions were observed). The picoeukaryotes (Phyto I and II) could not be classified due to their small cell size and limited contribution to FCM-C.
Similar to the average Chl-a concentration, mean phytoplankton abundance in S1 was higher than that in S2 (5.5 ± 3.0 vs. 3.7 ± 2.2 × 103 cells mL−1, n = 40 and 51, respectively, Online Resource 7). Overall, the contribution of nano-sized phytoplankton (Phyto IV–X) was 1.5 times higher in S1 compared to S2 (53 ± 24 and 35 ± 16%, n = 40 and 51, respectively), with Phyto IV, VI and IX dominating in S1 (13 ± 17, 24 ± 16 and 9 ± 16%, n = 40, respectively) and Phyto V in S2 (17 ± 13%, n = 51). All 10 phytoplankton clusters distinguished by FCM showed strong temporal dynamics with distinct differences between seasons (Fig. 6). At the start of the season during the NB period, the picoeukaryotic phytoplankton Phyto I and II were most abundant in S1 (45 ± 4% and 22 ± 3%, n = 3; Fig. 6a–c) and equally abundant to Phaeocystis Phyto III in S2 (25 ± 20, 26 ± 13, and 25 ± 14%, respectively, n = 5; Online Resource 8). Phyto I–III persisted during B1 in S1 (24 ± 19, 31 ± 11 and 15 ± 8%, respectively, n = 9), while diatom Phyto V bloomed during this period in S2 (30 ± 10%, n = 15; Fig. 6e). Phyto IX (diatom) became also abundant during B1 of both seasons, contributing up to 18% in S1 and 45% in S2 (Fig. 6i and Online Resource 8). The B2 period of S1 was dominated by cryptophytes (Phyto IV 26 ± 21%, n = 16; Fig. 6d and Online Resource 7) and diatom Phyto VI (26 ± 14%, n = 16; Fig. 6f), whereas Phaeocystis Phyto III and diatom Phyto V had the largest share in S2 (51 ± 14% and 16 ± 7%, respectively, n = 17; Fig. 6c, e). During the initial stage of the large phytoplankton bloom in B3 of S1 (Fig. 4a), P. antarctica and diatom group Phyto VI were most abundant (contributing up to 23 and 56% of total abundances, respectively; Fig. 6c, f, Online Resource 8). The larger diatom group Phyto IX (11.5 ± 3 µm, n = 15) succeeded, making up to 64% of total abundance (Fig. 6i). Unlike S1, total phytoplankton abundances during B3 in S2 were relatively low (mean 5.1 ± 3.4 and 1.9 ± 1.2 × 103 mL−1, n = 40 and 51, respectively) and mostly dominated by Phyto III (44 ± 24%, n = 51).
The CCA of FCM abundances revealed that the models shown in Fig. 5b, c explained 66% of the variation in the dataset of S1 (33% and 25% by first two axes) and 71% of S2 (35 and 22% by first two axes explained). Contributing to the formation of both axes during both seasons were ice type (S1 p < 0.001, n = 40; S2 p = 0.010, n = 51), temperature (S1 p < 0.001, n = 40; S2 p < 0.001, n = 51), PAR (S1 p < 0.001, n = 40; S2 p = 0.008, n = 51) and salinity (S1 p < 0.001, n = 40; S2 p < 0.001, n = 51), followed by phosphate (S1 p < 0.001, n = 40; S2 p < 0.001, n = 51), and also for S1 nitrate (S1 p < 0.001, n = 40) and S2 Zeu/15 m (S2 p < 0.001, n = 51). Phyto I, II, VIII and X in S1 were associated with fast ice, as well as high salinity and low temperature. In S2, ice type (grease ice) was again associated with Phyto I and II, but also diatoms Phyto VI and VIII. Additionally (in S2), these phytoplankton clusters were associated with high salinity, PAR, Zeu/15 m and phosphate. Phyto X in S2 was, together with other diatom clusters, Phyto V, VII and IX, associated with low PAR and low Zeu/15 m conditions (Fig. 5c). Phyto IX in S1 was also correlated with low PAR and low phosphate concentrations, the predominant environmental conditions during B3 in S1 (open triangles in Fig. 5b). Phyto IV (cryptophytes) in S1 was associated with high temperature, PAR and phosphate conditions (as for example found during B2 in S1; open circles Fig. 5b). In S2, these cryptophytes, as well as Phaeocystis (Phyto III), were similarly associated with high temperature and high PAR, but also low salinity and low phosphate (Fig. 5c).
Considering the variation in cell sizes, we converted both phytoplankton abundances and Chl-a to cellular carbon for a more detailed comparison (Fig. 7a, b). As to be expected, the larger-sized phytoplankton clusters made up most of the cellular carbon (FCM-C) during both seasons (Fig. 8a, b), despite occasional low abundances (e.g. diatom Phyto X during March in S2; Fig. 6j). Due to size restrictions of FCM analysis (reliable acquisition is limited to cells around 20 µm in diameter, based on the laser beam width), we focused our comparison of FCM-C with CHEMTAX-C on the ≤ 20 µm size fraction. The < 5 µm and 5–20 µm fractions showed generally good agreement for both seasons (Fig. 7c–f). The few discrepancies were related to FCM population-specific variations in cell diameter over time, whereby the actual diameter of the dominant population, at that specific moment in time, was larger than the mean. A larger diameter (compared to the mean) combined with high abundance resulted in observably lower FCM carbon estimations when using mean cell size compared to the actual cell size at the time.
When taxonomic composition was expressed in Chl-C, 42% of variation was explained by the CCA model shown in Fig. 9a (40 and 1% by first 2 axes). In particular, Cryptophyceae were associated with the main environmental variables contributing to the formation of the two primary axes, i.e. higher temperature (p < 0.001, n = 101), a reduced potential for light limitation (higher Zeu/15 m, p < 0.001, n = 101) and higher phosphate concentrations (p = 0.002, n = 101). The CCA based on FCM-C in S1 showed similar clear clustering of cryptophytes Phyto IV with B2 environmental data points when temperature was highest (Fig. 9b). Besides temperature, Phyto IV also correlated with higher PAR in both S1 and S2 (Fig. 9b, c). The FCM-C-based CCA showed that the prymnesiophytes and Phyto III also related strongly to higher PAR in S1 and high PAR, high Zeu/15 m, and relatively low salinity in S2. The different diatoms did not display similar relationships based on FCM-C. Phyto V, VII, and VIII were all associated with high PAR in S1, and ice type especially in S2 (Phyto VI and VIII with grease and Phyto V and VII with pack ice; Fig. 9b, c). With the FCM-C-based CCA model, 42% of variation in the dataset of S1 was explained by the environmental variables with the first 2 axes explaining 31 and 9%, respectively. During S2, the CCA model explained even more, i.e. 65% of total variation in FCM-C with the first two axes explaining 40 and 16% of variation, respectively.
Ice type and early season phytoplankton dynamics
Previous studies have shown that melting sea ice can seed the surrounding waters with phytoplankton cells (e.g. Garrison et al. 1987; Arrigo 2003; Jin et al. 2007), however, there is currently a limited understanding how ice type can structure phytoplankton community dynamics. Our data indicate that ice type (fast, grease, pack or brash ice) was an important factor structuring the pre-bloom phytoplankton community and the cell size structure of the early summer phytoplankton bloom community (Figs. 5, 9). During the pre-season (August to October, data not shown) ice cover was similar between the 2 years; however, the pre-bloom phytoplankton community of S1 was associated with fast ice, while grease ice was important during S2 (Figs. 5, 8). Ice type rather than ice cover seemed the most influential factor establishing the seed population for the productive season. The initial summer phytoplankton bloom (B1) during both seasons (Fig. 4) coincided with the period of greatest increase in vertical stratification (Eveleth et al. 2017). Nevertheless, decreasing fast ice cover in S1 (Fig. 2) coincided with a bloom of large diatoms (> 20 µm), while in S2, the B1 bloom consisted of diatoms mostly ≤ 20 µm (Online Resource 4) which corresponded to an increase in brash ice (turning into pack ice). Distinct differences in the pigment to Chl-a ratios during S1 and S2 are indicative of dissimilar phytoplankton seeding from ice. The relatively low ratios of Chl-c2, fucoxanthin and diadinoxanthin + diatoxanthin [Dd + Dt] to Chl-a (0.1, 0.5 and 0.1, respectively; Online Resource 9a) during B1 in S1 indicate that the larger diatoms were the result of marginal ice edge algal blooms (Rodriguez et al. 2002; Wulff and Wängberg 2004; Hashihama et al. 2008; Kozlowski et al. 2011). In contrast, the higher Chl-c2 and fucoxanthin to Chl-a ratios (1.4 and 2.5, respectively, Online Resource 9b) during the initial phytoplankton biomass rise in S2 suggests that the smaller-sized diatoms had higher light absorption efficiencies in the blue spectrum (characteristic of ice-associated algae; Robinson et al. 1995). Furthermore, the higher Dd + Dt to Chl-a ratio of 1.2 indicates these diatoms were recently released from the photo-protective effect of ice and became exposed to high surface light (Robinson et al. 1997; Petrou et al. 2011; Van De Poll et al. 2011).
Summer phytoplankton dynamics
The increased Chl-a concentrations during B1 in both seasons coincided with rapid declines in PAR (to potentially limiting levels; Fig. 3d) most likely due to the increasing light attenuation (community shading). The low light availability was associated with a shift towards smaller-sized diatoms (Timmermans et al. 2001), particularly Phyto IX (Fig. 6i). Whereas additional nutrient depletion may have caused the decline of the B1 bloom in S1, a short-lived moderate mixing event end of December of S2 (Online Resource 10) resulted in elevated nutrient concentrations and sustained phytoplankton standing stock during the low salinity-induced highly stratified (Gonçalves-Araujo et al. 2015; Rozema et al. 2017b) B2 period (Online Resource 3, Figs. 3b and 2c). Subsequently, rapid nutrient drawdown may have caused growth-limiting conditions during early February (0.04 and 0.03 µM, for phosphate and nitrate respectively); however, a mixing event around that time (represented here for example by increased salinity, Fig. 3b) quickly reintroduced nutrients into the euphotic zone and sustained high proportions of large diatoms (Fig. 4b and Online Resource 4b: data on 12 Feb).
In contrast to S2, the B2 period in S1 was largely dominated by Cryptophyceae (Fig. 4), which were found to be associated with high temperature and light availability (Figs. 5, 9). Temperature and light have previously been reported as the most likely factors promoting Cryptophyceae in the WAP (Kopczynska 1992), and Buma et al. (1993) reported maximum division rates of Antarctic cryptophytes at 1 °C and 50 µmol quanta m−2 s−1, similar to B2 in S1 of this study. Mendes et al. (2017) also described strong positive correlations between cryptophytes and temperature in WAP waters. Although some studies linked reduced salinity with cryptophytes (Buma et al. 1992; Moline et al. 1997, 2004; Mendes et al. 2013), our study displays only a weak association with salinity (Figs. 5, 9). It may be that previous associations of cryptophytes with salinity were largely driven by collinearity between salinity and temperature. Alternatively, differences in species-specific responses to environmental variables could also be responsible for the variances observed (Henley et al. 2019).
Phaeocystis (Phyto III) was one of the most abundant FCM groups consistently present during both seasons (Fig. 6c). Phyto III dynamics were largely associated with light availability (PAR and Zeu/15 m) and salinity, factors also important for Prymnesiophyceae (Figs. 5, 9), with the highest abundances occurring during a period of relatively low salinity (B2 in S2; Figs. 6c, 3b). Phaeocystis antarctica has been reported to tolerate low salinity better than high salinity (Bates and Cota 1986; Van Leeuwe et al. 2014) and display decreased photosynthetic activity in response to higher salinity and lower temperatures (Kennedy et al. 2012). Additionally, P. antarctica appears to have efficient photosystem and photo-damage repair mechanisms, enabling it to grow at higher PAR and in well-mixed waters (Kropuenske et al. 2009; Alderkamp et al. 2012). Finally, P. antarctica growth rate has been reported to increase with the temperature (Schoemann et al. 2005; Rose et al. 2009; Lee et al. 2016), supporting our finding that Phyto III is also associated with the increasing temperature.
Towards the end of the productive season (B3 period), a large and prolonged bloom of nano-sized diatoms (Phyto VI and IX; Fig. 6f, i) was observed in S1 but not present in S2. Phyto VI correlated with relatively high temperature, PAR and phosphate (sustained by deeper mixing; Figs. 2d, 5, and 9). As Phyto VI peaked in abundance, PAR declined, light became potentially limiting, and the shallowed MLD resulted in a rapid decrease in phosphate. Subsequently, Phyto IX bloomed under conditions of reduced phosphate (however sustained by regular mixing) and low light availability (< 3 µmol quanta m−2 s−1). Blooms of Phyto IX only occurred when biomass accumulation reduced light to potentially limiting levels. Conversely, higher light conditions in S2 may have reduced Phyto IXs competitive advantage under low light and restricted bloom development when PAR and Zeu/15 m were higher (Fig. 2c, d). Specifically during B3 in S2, low temperature may have restricted the accumulation of Phyto VI (Suzuki and Takahashi 1995; Montagnes and Franklin 2001) and consequently the relatively reduced light attenuation (lack of community shading) would have prevented Phyto IX to bloom and increase Chl-a concentrations further.
The environmental variables were unable to explain all of the variabilities in phytoplankton abundance and community composition in Ryder Bay. The remaining variation is likely an indication for the importance of loss factors in structuring phytoplankton communities (Yang et al. 2016; Mojica et al. 2016). Biomass accumulation is after all the net result of production (regulated by physical and chemical variables) and loss rates such as grazing and viral lysis. The decline in phytoplankton biomass in S2 mid-February (end of B2) and the reduced Chl-a concentrations during B3 (compared to S1) may have been, at least partly, due to relatively high grazing pressure. Meso-zooplankton numbers peaked just before the start of the B3 period in S2, whereas numbers were declining at the same time in S1 (Online Resource 11). For both seasons, the period with enhanced zooplankton standing stock coincided with a distinct rise in ammonium concentrations. Although the temporal dynamics of ammonium seems related to mixing events, similar to the other macronutrients (Online Resource 3), micro- and meso-zooplankton are known to excrete ammonium (Goeyens 1991; Brussaard et al. 1996; Atkinson and Whitehouse 2000).
The B2 period in S1 was cryptophytes-dominated with relatively low abundances of diatoms. Krill have been shown to selectively graze diatoms, rather than cryptophytes or prymnesiophytes, even when diatoms were rare (Verity and Smayda 1989; Head and Harris 1994; Haberman et al. 2003). Furthermore, Kopczynska (1992) showed that in WAP coastal waters, low biomass areas dominated by flagellates also host dense krill swarms. This suggests that water column stability and zooplankton grazing act together to regulate phytoplankton community structure by reducing the biomass of diatoms and may suppress the development of a phytoplankton bloom. Besides grazing, viral lysis may contribute to the selective removal of phytoplankton (Brussaard 2004), influencing both species and strain diversity. Furthermore, high temperatures during B2 of S1 may have promoted phytoplankton losses due to viral lysis, related to a shorter virus latent period and increased burst size (Maat et al. 2017; Piedade et al. 2018).
The combined approach of using FCM (abundances), CHEMTAX (taxonomic composition) and size structure provides a more detailed understanding of the structure and composition of natural phytoplankton communities. Together with multivariate statistics, these methods increased the size spectrum of the study community and enabled the differentiation and comparison of individual size classes and chemotaxonomy within different bloom periods, as well as identifying physicochemical associations. This enabled predictions regarding the taxonomy of various phytoplankton groups identified by FCM (e.g. prymnesiophyte Phyto III) and allowed for a better discrimination within an individual taxonomic group (i.e. diatom populations Phyto V–X). Diatoms dominated the biomass generally throughout both seasons and in all size classes, however, Chl-a-based CCAs could not assign strong drivers to this group. It can be expected that each size class (and each population within that size class) is driven by different environmental variables, preventing the assignment of reliable associations to this diverse taxonomic group. This oversimplification was avoided by defining populations via FCM which provided the greater resolution needed to understand the relationship between populations and environmental factors.
The current study provides a high-resolution temporal description of phytoplankton, particularly the pico- and nano-size fractions, and the physical and chemical characteristics over two distinct productive seasons. Multivariate analysis revealed that ice type was the most influential differential factor on phytoplankton community composition during spring and early summer, whereas temperature, light, phosphate and salinity played a more influential role during late summer and autumn. Ice type rather than ice cover structured the pre-bloom phytoplankton community as well as the size class of the summer phytoplankton bloom. Maximum biomass accumulation was regulated by light and nutrient (mainly phosphate) availabilities which in turn were regulated by wind-driven mixing events. Prolonged salinity-driven stratification combined with moderate mixing and seawater temperature > 0 °C (supplying DFe from ice melt) coincided with the development of a large (> 20 µm) diatom-dominated phytoplankton community. Flagellates were associated with late summer conditions of high temperature (Cryptophyceae), low salinity and high light availability (Prymnesiophyceae) and would likely be more dominant under a warmer future climate with earlier and prolonged stratification (Falkowski and Oliver 2007). In a future ‘warmer’ autumn, which follows on from a ‘warmer’ summer, we would expect to see an increased frequency of large and prolonged nano-sized diatom blooms as observed during B3 in S1. To improve the variance explained by Chl-a-based CCAs, we recommend performing frequent Chl-a fractionations. One caveat is that multiple FCM groups can fall into the same Chl-a size fraction, and if driven by different factors, this would lead to confounding results. FCM, however, provides fundamental information (for the ≤ 20 µm size fraction) on the abundances of the various populations while enhancing the ability to differentiate important physicochemical correlations with phytoplankton community structure and thus provides a vital tool for studying phytoplankton dynamics. The addition of large cell flow cytometry and high through-put sequencing of sorted phytoplankton populations (Eiler et al. 2013; Johnson and Martiny 2015; Massana et al. 2015; Visco et al. 2015), would enhance analysis of the phytoplankton community.
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We wish to thank the British Antarctic Survey for their logistical support and cooperation during the field campaign. This work was part of the ANTPHIRCO project (grant 866.10.102 awarded to C.P.D.B.) which was supported by the Earth and Life Sciences Foundation (ALW), with financial aid from the Netherlands Organisation for Scientific Research (NWO). Furthermore, we wish to thank Zoi Farenzena and Dorien Verheyen for their help and support during the field campaign as well as Swier Oosterhuis and Anna Noordeloos for their technical support at the Royal Netherlands Institute for Sea Research (NIOZ).
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Biggs, T.E.G., Alvarez-Fernandez, S., Evans, C. et al. Antarctic phytoplankton community composition and size structure: importance of ice type and temperature as regulatory factors. Polar Biol 42, 1997–2015 (2019). https://doi.org/10.1007/s00300-019-02576-3
- Cellular carbon
- Flow cytometry
- Ice type
- Size fractionation