Ocean acidification substantially alters ocean carbon chemistry and hence pH but the effects on sea ice formation and the CO2 concentration in the enclosed brine channels are unknown. Microbial communities inhabiting sea ice ecosystems currently contribute 10–50% of the annual primary production of polar seas, supporting overwintering zooplankton species, especially Antarctic krill, and seeding spring phytoplankton blooms. Ocean acidification is occurring in all surface waters but the strongest effects will be experienced in polar ecosystems with significant effects on all trophic levels. Brine algae collected from McMurdo Sound (Antarctica) sea ice was incubated in situ under various carbonate chemistry conditions. The carbon chemistry was manipulated with acid, bicarbonate and bases to produce a pCO2 and pH range from 238 to 6066 µatm and 7.19 to 8.66, respectively. Elevated pCO2 positively affected the growth rate of the brine algal community, dominated by the unique ice dinoflagellate, Polarella glacialis. Growth rates were significantly reduced when pH dropped below 7.6. However, when the pH was held constant and the pCO2 increased, growth rates of the brine algae increased by more than 20% and showed no decline at pCO2 values more than five times current ambient levels. We suggest that projected increases in seawater pCO2, associated with OA, will not adversely impact brine algal communities.
Citation: McMinn A, Müller MN, Martin A, Ryan KG (2014) The Response of Antarctic Sea Ice Algae to Changes in pH and CO2. PLoS ONE 9(1): e86984. https://doi.org/10.1371/journal.pone.0086984
Editor: Kerrie Swadling, University of Tasmania, Australia
Received: August 21, 2013; Accepted: December 19, 2013; Published: January 28, 2014
Copyright: © 2014 McMinn et al. This is an open-access article distributed under the terms of the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original author and source are credited.
Funding: Financial support for this project came from the Australian Antarctic Division (AAS 4008) and the Australian Research Council (ARC) Discovery Project DP1093801. The funders had no role in study design, data collection and analysis, decision to publish, or preparation of the manuscript.
Competing interests: The authors have declared that no competing interests exist.
Ocean acidification (OA) is a direct ocean response to anthropogenic CO2 emissions and will continue irrespective of whether the planet warms. The increase in atmospheric CO2 levels from the present (∼400 µatm) to levels likely by the end of the century (∼700 µatm, ), will lead to an increase in average seawater CO2 concentration from around 12.5 µmol kg−1 to ∼20 µmol kg−1. This will be accompanied by a fall in pH from a global preindustrial average of ∼8.2 to 7.8. Current pH values adjacent to Antarctica are 8.019–8.045 . Some microalgal species will benefit from increased CO2 concentrations, which will facilitate faster rates of photosynthesis and growth. Although many species, including most diatoms, possess effective carbon-concentrating mechanisms (CCM), they may still benefit from decreased costs for carbon acquisition , , . Whether global marine primary production will benefit from projected changes in CO2 levels will largely be determined by nutrient supply and grazer impact since most oceans are oligotrophic and limited by nutrients and/or light rather than CO2 availability , , , .
The direct effect of oceanic pH on microalgal cells is less clear but recent work has demonstrated that it can modify intracellular pH and affect membrane potential, energy partitioning and enzyme activity , . Many coastal and estuarine phytoplankton are unaffected by external pH changes in the range 7.8–8.5, probably because this range reflects natural diurnal and seasonal changes in many coastal environments , , . Natural increases in pH to >10 have been reported from dense phytoplankton blooms before limiting access to CO2 causes photosynthesis to be impaired. Furthermore, microalgae living in extreme environments are able to tolerate short term exposure over a very large range in pH (3–11)  but in the ocean it is likely to be the resultant changes in nutrient availability and not pH itself, which will have the greatest impacts on growth and survival .
The situation in sea ice ecosystems, however, is quite different to that in the open sea. During ice formation, internal gas concentrations are heavily modified by exclusion of gases from the ice crystal structure. This results in a steep decline in pH, changes to gas solubility at high salinity and low temperature often resulting in supersaturation and outgassing . Internal liquid seawater temperatures can drop to below −15°C with salinities fluctuating between 173 in winter and 0 in summer . Photosynthetic activity has been recorded at temperatures below −10°C . However, in spring and summer this trend is usually overridden by the photosynthetic activity of dense microalgal communities that cause the pH to rise as a result of the depletion of the dissolved CO2. Values of up to 8.9, for instance, have been reported from platelet ice  and up to 9.9 in brine channels within the ice matrix .
Sea ice microbial communities are a critical component of polar marine ecosystems, contributing 10–50% of the annual primary production of polar seas , supporting overwintering zooplankton species, especially Antarctic krill, and seeding spring phytoplankton blooms. Ocean acidification will be experienced most strongly in these ecosystems and is likely to have significant effects on all trophic levels . These communities are a close association between microalgae, heterotrophic bacteria and heterotrophic protists. Algae and other microorganisms proliferate in sea-ice during spring with bacterial production coupled tightly to algal production . In some communities, such as those at the surface of the ice or those in brine channels, cells grow despite exposure to extremes of temperature and salinity, while those on the underside of the ice remain at close to freezing point. Brine channel and surface communities have only limited access to the underlying water column and consequently their CO2 (and nutrient) supply becomes severely restricted. Under these circumstances, restricted CO2 supply limits microalgae growth . Thus, unlike planktonic ecosystems where CO2 is rarely in short supply, in sea ice brine systems the shortage is often acute and the addition of CO2 as a result of OA may partially alleviate this stress. Nitrate also becomes less significant as ammonium levels increase at lower pH with enhanced disassociation to ammonia, which is more readily assimilated . In addition, elevated oxygen levels may negatively influence growth  as do processes associated with iron and nitrogen transformation . By comparison, algal communities on the undersurface of the ice usually experience replete nutrient conditions and an unrestricted CO2 supply. Sea ice microbial communities are already living at physiochemical extremes and additional changes such as a decrease in pH have the potential to shift environmental conditions beyond physiologically tolerable levels.
At its most fundamental level, ocean acidification is about the effects of changing resource availability (i.e. nutrients and CO2) coupled with cellular energy demands and environmental changes in pH. Here we report the in situ response of ice algal communities to changing carbonate speciation. This study is the first in situ study of the response of sea ice brine algae to manipulated carbon chemistry.
Materials and Methods
The sea ice incubation experiments were conducted on 16–26 Nov, 2012 at Cape Evans, McMurdo Sound (77° 38′S, 166° 24′E), Antarctica. Brine was collected from 0.5 m deep sack holes, drilled with a 20 cm diameter motorised auger at the beginning of each experiment (Jiffy, USA). The temperature and salinity of the brine was measured prior to chemical manipulation and preparation of each treatment, using a digital thermometer (Digitron, 2098T) and a refractometer (HANNA Instruments Inc. Woonsocket-RI-USA, Model: HI96822). After chemical manipulation (see below), five replicates were decanted into clear 250 ml polycarbonate vials with clear lids leaving no headspace. The vials containing the brine algae were placed in 13 cm diameter holes that had been cored to a depth of 0.5 m with a motorised ice corer (Kovacs, USA). The ice cores initially extracted from each hole was subsequently placed on top of the vials, generating a natural light and temperature environment. Irradiance was measured with a Biosphaerical QSP 200 4π light meter.
The work program and sampling protocol for these experiments were approved under the provisions of the Antarctic Treaty by a permit (issued to Ken Ryan) by Antarctica New Zealand. No protected or endangered species were used in the experiments and no specially protected areas were visited. All experiments were conducted in situ, in Antarctica.
The, brine carbonate chemistry was manipulated by the addition of HCl, NaOH and NaHCO3. In the first experiment (5 treatments and 5 replicates), total alkalinity (TA) was manipulated while keeping the DIC concentration constant by the addition of HCl or NaOH resulting in a pH (total scale) and pCO2 gradient from 7.19 to 8.66 and from 178 to 5095 µatm, respectively. In the second experiment (4 treatments and 5 replicates), the carbonate system was manipulated by addition of NaHCO3 and NaOH keeping the pH constant (8.02±0.05) while applying a pCO2 gradient ranging from 505 to 2477 µatm.
Samples for dissolved inorganic carbon (DIC) and TA were taken from the bulk samples at the beginning of each experiment and then from the replicates at the end. Samples were taken for DIC, TA, chl-a, Coulter Multisizer-analysis and PAM fluorometry at the beginning and end of each experiment. DIC samples were filtered through a sterile filter (pore size 0.2 µm) into 12.5 ml Labco Exetainers® avoiding air contact, poisoned with HgCl2 and sealed air tight. TA samples were filtered through GF/F filters (used for chl-a analysis), poisoned with HgCl2 and stored in 250 ml polyethylene flasks. Samples for Coulter-Multisizer analysis (12 ml) were fixed with Lugol’s solution and stored in the dark until analysed.
The carbonate system was calculated from temperature, salinity, TA and DIC measurements using the program CO2sys (version 1.05 by E Lewis and DWR Wallace) with dissociation constants for carbonic acid . DIC and TA samples were analysed as the mean of triplicate measurements with the infrared detection method using an Apollo SciTech DIC-Analyzer (Model AS-C3) and the potentiometric titration method with modification for high alkalinity ,  respectively. Data were corrected to Certified Reference Materials (CRM) (Scripps Institution of Oceanography, USA). Consecutive measurements of the Dickson standard resulted in an average precision of >99.9% for both TA and DIC analysis.
Coulter Multisizer Analysis
Samples were analysed as the mean of triplicate measurements with a Beckman Coulter Multisizer IV equipped with a 100 µm aperture covering particle volume range from 4 to 113,097 µm3.
Chlorophyll Analysis and Flourometry
Samples were filtered onto 42 mm diameter Whatman GF/F filters. The filters were then extracted in 10 ml of 90% methanol for 12 hours at 4°C in the dark. Chlorophyll-a was measured on a Turner 10AU fluorometer using the acidification method .
A WaterPAM (Walz GmbH, Germany) was used for the maximum quantum yield (Fv/Fm) measurements. Gain settings were between 18 and 22. All samples were dark adapted at −2°C for one hour prior to measurement. One-way ANOVA was used to compare end-point data for the control and treatment.
The sea ice at Cape Evans, McMurdo Sound, in November-December 2012 was 1.7 m thick with no snow cover. The brine community was strongly dominated by the dinoflagellate, Polarella glacialis. Maximum midday irradiances were approximately 100–120 µmol photons m−2 s−1 in the 50 cm deep holes.
Reduced pH and Increased CO2 Experiment
Initial brine salinity was 65 and the temperature was −3°C. Initial pH and pCO2 were 7.84 and 1288 µatm respectively. Manipulated pH and pCO2 were between 8.53 to 7.11 and 238 µatm to 6066 µatm respectively (Table 1). Initial chl-a concentration in the brine was 0.553±0.058 µg chl-a l−1 and the initial biovolume of microalgae was 1.36×105 µm3/ml. Growth rate estimates from biovolume were consistently higher than estimates from chlorophyll measurements but indicated a similar trend with highest growth rates at pH = 8.37 and lowest at pH = 7.19 (Figure 1a). Initial Fv/Fm was 0.32±0.02. At the end of the incubation values ranged from 0.30±0.15 at pH 7.19 to 0.57±0.09 at pH = 8.66 (Figure 2a) but these differences were not significantly different (p>0.05).
a: Growth rate of the brine algal incubations with varying pH, based on changes in chl-a and biovolume, in November 2012, experiment 1. b: Growth rate of the brine algal incubations (chlorophyll a and biovolume) with constant pH and varying CO2 in November 2012, experiment 2. Vertical grey line signifies initial pH and pCO2.
a: Maximum quantum yield (Fv/Fm) of the brine algal incubations with varying pH in November 2012, experiment 1. b: Maximum quantum yield (Fv/Fm) of the brine algal incubations with constant pH and varying CO2 in November 2012, experiment 2. Vertical grey line signifies initial pH and pCO2.
Constant pH (8.02) and Increased CO2 Experiment
Initial brine salinity was 54 and brine temperature was −2.5°C. Initial pH and pCO2 were 8.02 and 587 µatm respectively. Manipulated pH remained constant at approximately 8.0, manipulated pCO2 varied between 587 and 2464 µatm (Table 1). Initial chl-a concentration was 5.031 µg chl-a l−1 and the initial microalgal biovolume was 4.97 106 µm3/ml. Estimated growth rates from chlorophyll and biovolume measurements increased with pCO2 (Figure 1b). Fv/Fm exhibited no significant difference with respect to CO2 concentration (p>0.05, Figure 2b).
OA produces both a drop in pH (and calcium carbonate saturation state) and a rise in CO2 concentration and these changes produce quite different results. While a decline in calcium carbonate saturation state primarily impacts calcifiers, an increase in CO2 availability potentially impacts photosynthesis in all autotrophs , . Bach et al.  attempted to isolate the effects of reduced pH and elevated pCO2 on the calcifier, Emiliaia huxleyi. They found that growth rates were directly related to CO2 at low pCO2 but at higher CO2 levels they were adversely affected by associated decreases in pH. In the experiments described here, the carbonate chemistry was similarly manipulated to identify and then isolate the differing effects of reduced pH and elevated CO2 on sea ice brine communities.
The brine algal community was incubated under two different sets of conditions. In the first experiment the alkalinity remained constant and the pCO2 was manipulated without controlling the pH. This facilitated pH levels that ranged between 8.66 and 7.19 and pCO2 that ranged between 178 and 5095 µatm. Under these conditions growth was maximal at a pH of 8.39 (346 µatm). When the pH was held constant at ∼8.02 and the pCO2 manipulated, growth and Fv/Fm continued to increase from pCO2 of 505 µatm to 1780 µatm and then remained approximately constant up to 2477 µatm, i.e. growth reached a maximum at four times present atmospheric CO2 concentration and remained maximal to at least six times. The results presented here are consistent with those of Bach et al. , showing no change in growth rate with increasing CO2 at low concentrations but were adversely affected by decreasing pH (<∼7.2) at higher concentrations. These experiments showed that greater falls in pH to approximately 7.2 reduced the growth rate by almost 50%. However, if the pH remained at ∼8.0, increased CO2 resulted in a growth rate increase of approximately 20%.
Responses of microalgal taxa in OA experiments have been quite variable. Several recent studies have found that at elevated CO2 concentrations (up to 1000 µatm) photosynthesis and growth tends to increase at low irradiances but decrease at higher irradiances , , , . In particular, it has been found that elevated CO2 levels cause an onset of photoinhibition at lower irradiances . This response, however, is not universal. While many studies report that diatom growth rates respond positively to moderate increases in pCO2 , , , others showed little or no change , , , . With dinoflagellates also, many have shown little response to changes in pCO2 that are consistent with end of century scenarios .
Some of the taxon-specific differences in response are possibly associated with the possession of an effective carbon concentrating mechanism (CCM). These are widespread in diatoms , including sea ice diatoms , and have also been reported in some dinoflagellates , . However, it is not known whether a CCM is present in Polarella glacialis. Dinoflagellates are the only phytoplankton group that possesses form II Rubisco, which is mostly associated with anaerobic phototrophic bacteria, and has a particularly low affinity for CO2 . Without a CCM these organisms would experience growth-limiting concentrations of CO2 under current oceanic conditions  and for brine algae this would be exacerbated in the very high pH conditions often experienced in late spring and early summer. For P. glacialis to dominate these highly variable microenvironments, often with very low CO2 and O2 supersaturation, possession of an effective CCM would be highly likely.
Field studies in the Southern Ocean (Ross Sea) in an area of significant vertical mixing and Fe stress, however, showed a strong relationship between carbon uptake and elevated pCO2 . They also found that elevated pCO2 caused changes in species composition promoting the growth of large diatoms. Similar community composition shifts were also seen in field experiments in the equatorial Pacific .
Plankton communities that are naturally exposed to large variations in pH and CO2 concentration, such as brine algae, seem to have a greater tolerance to these changes. This has also been seen, for instance, in some coastal communities of the Baltic Sea ,  and North Sea  where natural pCO2 varies seasonally between 500 µatm and 2500 µatm. These communities demonstrated a high degree of tolerance and showed only subtle changes to elevated pCO2.
Importantly, future marine phytoplankton communities will not only be exposed to decreases in pH but also to coincident increases in abiotic factors such as temperature and light (though increased stratification) and it will be important to consider the cumulative effect of multiple ocean drivers , , . However sea ice microbial ecosystems are less likely to experience the same changes in abiotic factors as phytoplankton; temperature for instance can never rise beyond 0°C and except for local variations in light caused by snow cover and ice thickness, there are not likely to be significant changes in available light. Including co-varying manipulations of light and/or temperature in the experiments reported here was therefore less relevant than in planktonic systems.
Several of the experimental treatments reported herein experienced a loss of chlorophyll biomass (reported as negative growth rates) during the incubations. The most likely explanation for these decreases is grazing as light and temperature conditions remained unchanged and there is evidence from elsewhere that carbon manipulations do not affect the cellular chlorophyll content , , . There is, however, evidence that in some ecosystems changes in CO2 concentrations affects grazer-prey interactions . Although meiofaunal abundance within sea ice, and within brine channels in particular, is very low , , there are currently no published measurements of grazing rates. Change in chlorophyll biomass has often been used to measure growth in sea ice ecosystems (e.g. ) and there is an unstated assumption that grazing pressure remains constant. This assumption is probably reasonable in this study as incubation periods were relatively short. In this study growth rates were measured both by changes in chl-a and also by changes in biovolume. Although the two sets of measurements gave consistent trends, the estimates made by changes in biovolume were consistently higher. While the reason for this is uncertain, one explanation could be due to differential growth rates of different species of algae, e.g. if there were changes in the abundance of large celled diatoms with relatively low chl-a content per cell volume, then biovolume in the whole sample would increase at a greater rate than chl-a.
The experiments documented here demonstrate that sea ice brine algal communities are tolerant to the changes in pH that are likely to be experienced by the end of the century and will possibly benefit from the associated increases in CO2. However, physiological responses and expression of CCM activity are variable between species and even between strains of the same species . Also, the results reported here are based on short incubations and do not account for the ability of species and communities to adapt over longer time periods. It is probable that sea ice brine communities will not be adversely affected by OA.
Logistical support was provided by Antarctica New Zealand. A.-P. Zanandrea is acknowledged for her help with total alkalinity and Coulter Multisizer analysis.
Conceived and designed the experiments: AMcM. Performed the experiments: AMcM MM. Analyzed the data: AMcM MM AM. Contributed reagents/materials/analysis tools: AMcM MM KR. Wrote the paper: AMcM MM AM KR.
IPCC (2007).Climate Change: 2007: The Physical Basis. Cambridge University Press.
- 2. Matson PG, Martz TR, Hofmann GE (2011) High frequency observations of pH under Antarctic sea ice in the Southern Ross Sea. Antarctic Sci 23: 607–613.
- 3. Reinfelder JR (2010) Carbon concentrating mechanisms in Eukaryotic marine phytoplankton. Ann Rev Mar Sci 3: 291–315.
- 4. Riebesell U (2004) Effects of CO2 enrichment on marine phytoplankton. J Oceanog 60: 719–729.
- 5. Rost B, Zondervan I, Wolf-Gladrow D (2008) Sensitivity of phytoplankton to future changes in ocean carbonate chemistry: current knowledge, contradictions and research directions. Mar Ecol Prog Ser 373: 227–237.
- 6. Hutchins D, Mulholland MR, Fu F (2009) Nutrient Cycles and Marine Microbes in a CO2-Enriched Ocean. Oceanog 22: 125–145.
- 7. Giordano M, Beardall J, Raven JA (2005) CO2 concentrating mechanisms in algae: Mechanisms, Environmental Modulation, and Evolution. Ann Rev Plant Biol 56: 99–131.
- 8. Li G, Campbell DA (2013) Rising CO2 interacts with growth light and growth rate to alter Photosystem II photoinactivation of the diatom Thalassiosira pseudonana. PLoS ONE 8(1) e55562: Doi 10.1371/journal.pone.0055562.
- 9. de Kluijver A, Soetaert K, Czerny J, Schulz KG, Boxhammer T, et al. (2013) A C-13 labelling study on carbon fluxes in Arctic plankton communities under elevated CO2 levels. Biogeosci 10: 1425–1440.
- 10. Beardall J, Raven JA (2004) The potential effects of global climate change on microalgal photosynthesis, growth and ecology. Phycologia 43: 26–40.
- 11. Suffrian K, Schulz KG, Gutowska MA, Riebesell U, Bleich M (2011) Cellular pH measurements in Emiliania huxleyi reveal pronounced membrane proton permeability. New Phytologist 190: 595–608.
- 12. Rossol D, Sommer U, Winder M (2013) Community interactions dampen acidification effects in a coastal plankton system. Mar Ecol Prog Ser 486: 37–46.
- 13. Nielsen LT, Jakobsen HH, Hansen PJ (2013) High resilience of two coastal plankton communities to twenty-first century seawater acidification: Evidence from microcosm studies. Mar Biol Res 6: 542–555.
- 14. Berge T, Daugbjerg N, Anderson BB, Hansen PJ (2010) Effect of lowered pH on marine phytoplankton growth rates. Mar Ecol Prog Ser 416: 79–91.
- 15. Guyre RE, Konopka A, Brooks A, Doemel W (1987) Algal and bacterial activities in acidic (pH 3) strip mine lakes. Applied Environ Microbiol 53: 2069–2076.
Thomas DN, Dieckmann GS (2004) Sea Ice, an introduction to its physics, chemistry, biology and geology. Blackwell, Oxford, UK.
- 17. Ralph PJ, McMinn A, Ryan KG, Ashworth C (2005) Effect of salinity and temperature on the photokinetics of brine channel algae. J Phycol 41: 763–769.
- 18. Thomas DN, Kennedy H, Kattner D, Gerdes D, Gough C, et al. (2001) Biogeochemistry of platelet ice: Influence on particle flux under land fast sea ice during summer at Drescher Inlet, Weddell Sea, Antarctica. Polar Biol 24: 486–496.
- 19. Arrigo KR, Thomas DN (2004) Large scale importance of sea ice biology in the Southern Ocean. Antarctic Science 16: 471–486.
Royal Society (2005) Ocean acidification due to increasing atmospheric carbon dioxide. The Royal Society, London, 68pp (2005).
- 21. Kottmeier ST, Sullivan CW (1987) Late winter primary production and bacterial production in sea ice and seawater west of the Antarctic Peninsula. Mar Ecol Prog Ser 36: 287–298.
- 22. McMinn A, Skerratt J, Trull T, Ashworth C, Lizotte M (1999) Nutrient stress gradient in the bottom 5 cm of fast ice, McMurdo Sound, Antarctica. Polar Biol 21: 220–227.
- 23. McMinn A, Pankowski A, Delfatti T (2005) Effect of hyperoxia on the growth and photosynthesis of polar sea ice algae. J Phycol 41: 732–741.
- 24. Roy R, Roy L, Vogel K, Porter-Moore C, Pearson T, et al. (1993) The dissociation constants of carbonic acid in seawater at salinities 5 to 45 and temperatures 0 to 45°C. Mar Chem 44: 249–267.
- 25. Dickson AG, Afghan JD, Anderson GC (2003) Reference materials for oceanic CO2 analysis: A method for the certification of total alkalinity. Mar Chem 80: 185–197.
Bach LT, Bauke C, Meier KJS, Riebesell U, Schulz KG (2012). Influence of changing carbonate chemistry on morphology and weight of coccoliths formed by Emiliania huxleyi. Biogeosciences, 9, 3449–3463, 2012.
Evans CA, O’Reilly JE, Thomas JP (1987) A handbook for the measurement of chlorophyll a and primary production. College Station, Texas A&M University.
- 28. Beardall J, Stojkovic S, Larsen S (2009) Living in a high CO2 world: impacts of global change on marine phytoplankton. Plant Ecol Diversity 2: 191–205.
- 29. Bach LT, Riebsell U, Schulz KG (2011) Distinguishing between the effects of ocean acidification and ocean carbonation in the coccolithophore Emiliania huxleyi. Limnol Oceanog 56: 2040–2050.
- 30. Chen S, Gao KS (2011) Solar ultraviolet radiation and CO2-induced ocean acidification interacts to influence the photosynthetic performance of the red tide alga Phaeocystis globosa (Prymnesiophyceae). Hydrobiologia 675: 105–117.
- 31. Gao K, Helbling EW, Hader D-P, Hutchins DA (2012b) Responses of marine primary producers to interactions between ocean acidification, solar radiation, and warming. Mar Ecol Prog Ser 470: 167–198.
- 32. Gao KS, Xu JT, Gao G, Li YH, Hutchins DA, et al. (2012a) Rising CO2 and increased light exposure synergistically reduce marine primary productivity. Nature Climate Change 2: 519–523.
- 33. Wu Y, Gao K, Riebesell U (2010) CO2-induced seawater acidification affects physiological performance of the marine diatom Phaeodactylum tricornutum.. Biogeosci 7: 2915–2923.
Li G, Campbell DA (2013) Rising CO2 interacts with growth light and growth rate to alter photosystem II photoinactivation of the coastal diatom Thalassiosira pseudonana. PLOS One 8(1) e55562. doi:10.1371/journal.pone.0055562.
- 35. Kroeker KJ, Kordas RL, Crim R, Hendriks I, Ramajo L, et al. (2013) Impacts of ocean acidification on marine organisms: quantifying sensitivities and interaction with warming. Global Change Biol 19: 1884–1896.
- 36. Yang G Gao K (2012) Physiological responses of the marine diatom Thalassiosira pseudonana to increased pCO2 and seawater acidity. Mar Environ Res 79: 142–151.
- 37. Boelen P, van de Poll WH, van der Strate HJ, Neven IA, Beardall J, et al. (2011) Neither elevated nor reduced CO2 affects the photophysiological performance of the marine Antarctic diatom Chaetoceros brevis. J Exp Mar Biol Ecol 406: 38–45.
Crawfurd KJ, Raven JA, Wheller GL, Baxter EJ, Joint I (2011) The response of Thalassiosira pseudonana to long-term exposure to increased CO2 and decreased pH. PLOS One 6: Article Number: e26695 DOI: 10.1371/journal.pone.0026695.
- 39. Trimborn S, Breeeis T, Sweet E, Rost B (2013) Sensitivity of Antarctic phytoplankton species to ocean acidification: Growth, carbon acquisition, and species interaction. Limnol Oceanog 58: 997–1007.
- 40. Berge T, Daugbjerg N, Andersen BB, Hansen PJ (2010) Effect of lowered pH on marine phytoplankton growth rates. Mar Ecol Prog Ser 416: 79–91.
- 41. Tortell PD, Rau GH, Morel FM (2000) Inorganic Carbon Acquisition in Coastal Pacific Phytoplankton Communities. Limnol Oceanog 45: 1485–1500.
- 42. Mitchell C, Beardall J (1996) Inorganic carbon uptake by an Antarctic sea-ice diatom, Nitzschia frigida. Polar Biol 16: 95–99.
- 43. Rost B, Richter K-U, Riebsell U, Hansen PJ (2006) Inorganic carbon acquisition in red tide dinoflagellates. Plant Cell Environ 29: 810–822.
- 44. Brading P, Warner ME, Davey P, Smith DJ, Achterberg EP, et al. (2011) Differential effects of ocean acidification on growth and photosynthesis among phylotypes of Symbiodinium (Dinophyceae). Limnol Oceanog 56: 927–938.
- 45. Tortell PD, Payne CD, Li Y, Trimborn S, Rost B, et al. (2008) CO2 sensitivity of Southern Ocean phytoplankton. Geophys Res Lett 35: L04605
- 46. Tortell PD, DiTullio GR, Sigman DM, Morel FMM (2002) CO2 effects on taxonomic composition and nutrient utilization in an Equatorial Pacific phytoplankton assemblage. Mar Ecol Prog Ser 236: 37–43.
- 47. Dupont S, Pörtner H-O (2013) A snapshot of ocean acidification research. Marine Biol 160: 1765–1771.
- 48. Boyd PW (2013) Framing a biological response.s to a changing ocean. Nature Climate Change 3: 530–533.
- 49. Schrank-Schiel SB, Dieckmann GS, Gradinger R, Melnikov LA, Spindler M, et al. (2000) Meiofauna in sea ice of the Weddell Sea (Antarctica). Polar Biol 24: 724–728.
- 50. Krembs C, Gradinger R, Spindler M (2000) Implications of brine channel geometry and surface area for the interaction of sympagic organisms in Arctic sea ice. J Exp Mar Biol Ecol 243: 55–80.
- 51. Ryan KG, McMinn A, Hegseth EN, Davy SK (2012) The effects of ultraviolet-b radiation on Antarctic sea ice algae. J Phycol 48: 74–84.