Ice nucleating properties of the sea ice diatom Fragilariopsis cylindrus and its exudates
- 1Faculty of Chemistry, Bielefeld University, 33615 Bielefeld, Germany
- 2Faculty of Mathematics, Informatics and Natural Sciences, Universität Hamburg, 20354 Hamburg, Germany
- 3Department of Earth and Planetary Sciences, Weizmann Institute of Science, 76100 Rehovot, Israel
- aformerly at: Alfred Wegener Institute, Helmholtz Centre for Polar and Marine Research, 27568 Bremerhaven, Germany
Correspondence: Thomas Koop (email@example.com)
In this study, we investigated the ice nucleation activity of the Antarctic sea ice diatom Fragilariopsis cylindrus. Diatoms are the main primary producers of organic carbon in the Southern Ocean, and the Antarctic sea ice diatom F. cylindrus is one of the predominant species. This psychrophilic diatom is abundant in open waters and within sea ice. It has developed several mechanisms to cope with the extreme conditions of its environment, for example, the production of ice-binding proteins (IBPs) and extracellular polymeric substances known to alter the structure of ice. Here, we investigated the ice nucleation activity of F. cylindrus using a microfluidic device containing individual sub-nanolitre (∼90 µm) droplet samples. The experimental method and a newly implemented Poisson-statistics-based data evaluation procedure applicable to samples with low ice nucleating particle concentrations were validated by comparative ice nucleation experiments with well-investigated bacterial samples from Pseudomonas syringae (Snomax®). The experiments reveal an increase of up to 7.2 ∘C in the ice nucleation temperatures for seawater containing F. cylindrus diatoms when compared to pure seawater. Moreover, F. cylindrus fragments also show ice nucleation activity, while experiments with the F. cylindrus ice-binding protein (fcIBP) show no significant ice nucleation activity. A comparison with experimental results from other diatoms suggests a universal behaviour of polar sea ice diatoms, and we provide a diatom-mass-based parameterization of their ice nucleation activity for use in models.
Sea ice is a two-phase medium composed predominantly of crystalline ice with embedded liquid channels and pockets (inclusions) in which active life can take place. As seawater freezes, dissolved sea salt ions are segregated from the growing ice lattice and accumulate in liquid brine inclusions, which have a lower freezing point due to their high salinity. Its porous structure makes sea ice a habitat for various organisms and enables life within the liquid brine network. Higher irradiance levels in sea ice, when compared to the seawater column, represent an advantage for photosynthetically active microorganisms populating the pore space (Eicken, 1992). During sea ice formation, most microorganisms from the water column remain entrapped within the ice or are scavenged by floating ice crystals (Ackley and Sullivan, 1994). Species composition changes with the ageing of ice and the stabilization of the brine channel system (Krembs and Engel, 2001), resulting in a dominance of diatom species producing sticky extracellular polymeric substances (EPSs) with ice-adhering functions (Raymond et al., 1994).
The diatom Fragilariopsis cylindrus (see Fig. 1) is widespread in polar environments and is one of the predominant species within the Arctic and Antarctic microbial assemblages (Kang and Fryxell, 1992; Poulin et al., 2011; van Leeuwe et al., 2018). The species thrives within sea ice, where it can be found along the sea ice column (Bartsch, 1989; Garrison and Buck, 1989; Günther and Dieckmann, 2001; Poulin et al., 2011). It is, therefore, considered to be an indicator of sea ice extent in palaeoenvironmental studies for reconstructions of past variations (Gersonde and Zielinski, 2000). F. cylindrus is also abundant in the water column, for example, in the proximity of the sea ice edge zone (Kang and Fryxell, 1992; Lizotte, 2001) and in ice-covered waters (Garrison and Buck, 1989). F. cylindrus has developed a range of mechanisms for coping with the extreme conditions occurring within sea ice (Mock et al., 2017). One prominent example is the production of so-called ice-binding proteins (IBPs; Bayer-Giraldi et al., 2011) and of other EPSs that are also found in other diatom species (Wilson et al., 2015; Aslam et al., 2018). F. cylindrus produces several ice-binding protein (IBP) isoforms (fcIBPs), all of which belong to the broadly extended IBP family with a domain of unknown function DUF3494 (Vance et al., 2019). It was shown that fcIBP isoform 11 affects the microstructure, i.e. the shape and size, of ice crystals (Bayer-Giraldi et al., 2011, 2018). Moreover, EPSs offer a protective environment to F. cylindrus in order to cope with the conditions of the sea ice habitat (Aslam et al., 2012a, b, 2018). It has been suggested that fcIBPs accumulate in EPSs and, when in contact with the icy walls of brine inclusions, alter the pore space, resulting in an increased habitability (Bayer-Giraldi et al., 2011).
The very good ice-binding properties of fcIBP and EPSs (mainly polysaccharides and proteins) under sea ice brine conditions have been reported in previous studies (Krembs et al., 2002, 2011; Bayer-Giraldi et al., 2011). Ice-binding proteins (IBPs) bind to ice crystal surfaces and, by doing so, can control the crystal growth rate, inhibit ice recrystallization, or help to adhere their host to ice (Davies, 2014; Bar Dolev et al., 2016; Guo et al., 2017). Originally, IBPs were known as antifreeze (glyco)proteins, which protect fish and insects by thermal hysteresis, i.e. by depressing the temperature where active crystal growth occurs to below the equilibrium melting point temperature (Bar Dolev et al., 2016). However, not all IBPs have such thermal hysteresis antifreeze properties. For example, a recently discovered IBP from the Antarctic bacterium Marinomonas primoryensis binds its bacterial host to diatoms and the Antarctic sea ice layer (Guo et al., 2017). Furthermore, even ice nucleating proteins are sometimes considered to be a subgroup of IBPs because their active sites appear to be structurally similar, just much larger, than those of regular IBPs with antifreeze properties (Davies, 2014; Bar Dolev et al., 2016; Eickhoff et al., 2019; Hudait et al., 2019). These considerations may imply that the much smaller ice-binding sites of antifreeze IBPs could also stabilize the formation of small ice embryos and thereby promote the nucleation of ice from liquid water; however, this occurs only at very low temperatures (Davies, 2014; Bar Dolev et al., 2016; Eickhoff et al., 2019; Hudait et al., 2019). Indeed, it has been shown both experimentally and in molecular dynamics simulations that the ice-binding antifreeze proteins of the mealworm beetle Tenebrio molitor (tmAFP) can also trigger the nucleation of new ice crystals just a few degrees Celsius above the homogenous freezing temperature of water or an aqueous solution (Eickhoff et al., 2019; Hudait et al., 2019). Here, we explore whether a similar ice nucleating effect also occurs for IBPs from F. cylindrus.
Many biological particles such as bacteria, viruses, or diatoms have been detected in the sea surface microlayer and in the thawing permafrost (Leck and Bigg, 2005; Wilson et al., 2015; Irish et al., 2017; Creamean et al., 2020; Ickes et al., 2020; Roy et al., 2021). Some of these biological particles can increase the ice nucleation temperature of small water droplets and act as ice nucleating particles (INPs; DeMott et al., 2016; Ickes et al., 2020; Welti et al., 2020; Creamean et al., 2021; Hartmann et al., 2021; Roy et al., 2021). These biological particles can be transported to the atmospheric boundary layer by sea spray aerosol droplets (Irish et al., 2019; Steinke et al., 2022). In the polar atmosphere, they can be transported over long distances (Šantl-Temkiv et al., 2019, 2020). Sea spray aerosol contributes to ice nucleation under mixed-phase cloud conditions and at cirrus temperatures in the upper troposphere (DeMott et al., 2016; Hartmann et al., 2021; Wagner et al., 2021). Further experiments on diatoms and their EPSs show that they can promote ice nucleation in small droplets of water or seawater (Knopf et al., 2011; Wilson et al., 2015; Ickes et al., 2020; Xi et al., 2021). Thus, diatoms like F. cylindrus may affect ice nucleation in cloud droplets.
There are some differences regarding the relevance of INPs in the Arctic and Antarctic polar regions. While in both polar latitudes the absolute concentrations of INPs are low, the influence of anthropogenic aerosols and INPs is much larger in the Arctic due to long-range transport during the Arctic winter (Šantl-Temkiv et al., 2019, 2020; Ekman and Schmale, 2022). During the Arctic summer, aerosol lifetimes are shorter due to increased wet removal preventing long-range transport and thus increasing the importance of locally emitted INPs (Ekman and Schmale, 2022). In the Antarctic, the influence of anthropogenic aerosols and INPs is generally much smaller (Stohl and Sodemann, 2010; Ekman and Schmale, 2022). During winter, blowing snow from the sea ice is the main aerosol source in the southern polar region, while dimethyl sulfide and other organic compounds from algae blooms are the main source during summer (Ekman and Schmale, 2022).
In the following, we present experimental data on the ice nucleation activity of F. cylindrus diatom cells and their exudates. We then analyse and convert these data into a quantifiable format so that they can be compared to other measurements of this type. Finally, we provide a comparison to ice nucleation data of other polar diatoms together with a parameterization that generalizes their ice nucleation activity for use in atmospheric models.
2.1 Sampling and cultivation of the F. cylindrus diatoms
The investigated F. cylindrus cells belong to the strain TM99 isolated in 1999 from the sea ice of the Weddell Sea, Antarctica, by Thomas Mock (RV Polarstern ANT-XVI/3 expedition, which took place in the early spring from March to May 1999). Since then, stock cultures have been kept in medium (Guillard and Ryther, 1962) set up with Antarctic water and cultivated at 0 ∘C and under continuous illumination of approximately 25 µE m−2 s−1. Before the experiment, cell numbers of the F. cylindrus cultures were monitored using a Coulter counter, and cells were harvested during the exponential growth phase. Cell cultures were distributed in 50 mL Falcon tubes, each containing about 1×108 cells, and they were centrifuged at 0 ∘C at 3220 g for 30 min. The clear spent medium was carefully separated from the cell pellet by pipetting, and both were shock-frozen in liquid nitrogen and stored at −80 ∘C.
2.2 Sample preparation
2.2.1 Preparation of artificial seawater
For the ice nucleation experiments, we used artificial seawater that mimics the natural conditions in the habitat of Antarctic F. cylindrus diatoms. The salinity in the Antarctic region is about 34.5, which corresponds to 34.5 g salts dissolved in 1000 g seawater (Roy-Barman and Jeandel, 2016), and we prepared artificial seawater of this salinity for dispersing the diatoms and as a reference for the ice nucleation experiments. To prepare the seawater, the six most important ions were considered, i.e. the cations sodium, potassium, magnesium, and calcium and the anions chloride and sulfate, which together make up about 99.4 % of the dissolved ions in seawater (Roy-Barman and Jeandel, 2016). The composition of the salts and their concentrations are given in Table S1 in the Supplement. The artificial seawater was filtered through a syringe filter (0.22 µm; polyethersulfone; SimplePure) in order to exclude any effect of suspended dust particles on ice nucleation. This filter has been used for all filtrations in this study, unless otherwise mentioned. The samples were stored at a temperature of −18 ∘C before use.
2.2.2 Preparation of F. cylindrus samples
The initial F. cylindrus samples contained about 108 diatoms per tube (see Sect. 2.1). These samples were placed in a micro-reaction tube and were filled up with the filtered artificial seawater to a volume of 2 mL. The resulting stock suspension of 5×107 cells per millilitre was used in all experiments. By further dilution with filtered artificial seawater, we generated several more dilute suspensions with concentrations of 1×107, 2×106, 1×106, and 5×105 cells per millilitre. For ice nucleation experiments on the fragments and exudates of the F. cylindrus cells, we filtered these five samples.
In order to identify the ice nucleating entities of the F. cylindrus samples, we separated the different components by means of filtration and centrifugation. We filtered a 1×107 cells per millilitre F. cylindrus suspension, such that the F. cylindrus cells should remain in the filter, while smaller fragments of destroyed cells and any soluble species, such as soluble ice-binding protein fcIBP11, should be able to pass the filter (see Fig. S1 in the Supplement for details). Thereafter, we recovered the filter cake containing the whole F. cylindrus cells and larger cell fragments by shaking the filter in a vial with artificial seawater. Although we used the same volume of artificial seawater as for the preparation of the original cell suspension, we surmise that the concentration of the resuspended diatoms is lower than the initial concentration. From the comparison of the frozen fraction curves obtained with the sample with those of unfiltered samples (see below), our best estimate of the concentration is about 2×106 cells per millilitre (estimated uncertainty range 1×106–1×107 cells per millilitre). Finally, the cell suspension was filtered again for comparison with the pure artificial seawater sample. To verify the method, all steps were also done with a vial of pure artificial seawater without suspended F. cylindrus cells.
We also performed ice nucleation experiments on fresh medium (Guillard and Ryther, 1962) and on the spent medium in which the F. cylindrus diatoms were actually grown. The sample preparation procedure is described in detail in Fig. S2. The spent medium should not contain many cells because they were separated by centrifugation. Nevertheless, we filtered the medium, such that only small fragments and soluble proteins (e.g. fcIBP11) should have remained in the filtrate (Bayer-Giraldi et al., 2011). In the next step, this sample was centrifuged using a 100 kDa centrifugal filter (polyethersulfone; Sartorius Vivaspin 500; 15 000 g), such that the remaining solution should not contain any diatom fragments but only smaller soluble molecules such as the soluble fcIBP11 protein. For comparison, we also applied the identical centrifugation step with a freshly prepared medium that had never been in contact with any diatoms.
2.2.3 Preparation of P. syringae samples
In additional experiments, we verified our Poisson evaluation procedure (see Sect. 2.3.3). For this purpose, we used well-studied bacterial cells of P. syringae, commercially available as Snomax®, from the same batch as that investigated in previous studies (Budke and Koop, 2015; Wex et al., 2015). The molecular mass of the individual ice nucleating proteins in the bacteria is about 150 kDa (Wolber et al., 1986; Govindarajan and Lindow, 1988). A suspension of P. syringae, with a concentration of 4 mg mL−1, was prepared from dry Snomax® with double-distilled water. By diluting this stock suspension with further double-distilled water, we also prepared additional, more dilute suspensions with concentrations of , , and mg mL−1. Using an average value of the cell number density of 1.4×109 cells per milligram (Wex et al., 2015), these mass concentrations correspond to cell concentrations of 1.4×107, 2.8×106, and 1.4×106 cells per millilitre.
2.2.4 Preparation of fcIBP11
Previous studies suggest that fcIBP11 plays a major role in the response of F. cylindrus to freezing conditions (Bayer-Giraldi et al., 2010) by binding to the ice and affecting ice crystal growth (Bayer-Giraldi et al., 2011, 2018). For our experiments, we used the recombinant fcIBP isoform 11 (European Molecular Biology Laboratory, Heidelberg; GenBank accession no. DR026070). The protein was expressed, as previously described (Bayer-Giraldi et al., 2011), and resuspended in a Tris-HCl buffer (pH 7.0). To determine the ice nucleation activity of fcIBP11, we prepared a stock solution with a fcIBP11 concentration of 0.1 mmol L−1. We diluted this sample by a factor of 10 to a concentration of 0.01 mmol L−1, using a Tris-HCl buffer (pH 7.0), and performed ice nucleation experiments on both sample solutions with the modified WISDOM (WeIzmann Supercooled Droplets Observation on a Microarray) microfluidic experiment (Reicher et al., 2018; Eickhoff et al., 2019; see below).
2.3 Experimental methods for ice nucleation experiments
2.3.1 Differential scanning calorimetry
A classic method for the investigation of homogeneous and heterogeneous ice nucleation is differential scanning calorimetry (DSC) of emulsified droplets (Rasmussen and MacKenzie, 1972; Koop, 2004). Here, we used a DSC apparatus (TA Instruments; DSC Q100), which was described in detail previously, including its calibration procedure (Riechers et al., 2013). As bulk samples notoriously suffer from unwanted impurities, we performed measurements of inverse water-in-oil emulsion samples containing micrometre-sized droplets. As many thousands of droplets are investigated simultaneously, such samples allow the detection of very reproducible exothermic heterogeneous ice nucleation signals down to the homogeneous ice nucleation temperature of about −38 ∘C (Pinti et al., 2012; Riechers et al., 2013; Dreischmeier et al., 2017). Further information on the emulsion preparation procedure is given in the Supplement.
The DSC experiment has been used as a simple and direct method to check whether F. cylindrus diatoms are potential ice nucleators or not. The method does not allow for the observation of single droplets, and we can only study cell fragments, but not intact cells, because the latter are disrupted during the emulsion preparation process. Therefore, we have used the WISDOM microfluidic device, which is described below, as the main experimental method in this study.
2.3.2 WISDOM microfluidic device
Most of the ice nucleation experiments presented in this study were carried out using droplet microfluidics. In particular, we used a microfluidic device based upon the WISDOM experiment (Reicher et al., 2018, 2019), with some minor modifications for a set-up operated at Bielefeld University, including adapted temperature and heating rate calibrations (see a previous, detailed description; Eickhoff et al., 2019). These modifications and the general procedure for the sample preparation are given in the Supplement.
2.3.3 Evaluation procedure for samples with small INP concentrations
Ice nucleation studies using larger-volume droplet arrays usually employ relatively high concentrations of INPs per droplet, e.g. mineral dust particles or bacterial cells (Budke and Koop, 2015; Hiranuma et al., 2015, 2019; Wex et al., 2015; DeMott et al., 2018; Kunert et al., 2019; Ickes et al., 2020) to ensure that freezing is induced at a temperature that is higher than that triggered by the supporting surface or minute numbers of impurities contained in the water. In the present study, the total number of INPs was small due to the limited availability of F. cylindrus cells, suggesting the use of small droplet methods which require less total INP material. We investigated droplets with a diameter of 90 µm, corresponding to a volume of about 380 pL. Another, probably more important, advantage of using these small droplet volumes is that we can measure ice nucleation down to the homogenous freezing temperature of water (Riechers et al., 2013; Reicher et al., 2018; Tarn et al., 2021), also enabling the investigation of rather poor ice nucleators. As the concentrations c of F. cylindrus cells varied between 5×105 and 5×107 cells per millilitre, the corresponding average INP concentrations ranged between 0.19 and 19 diatom cells per droplet. It becomes immediately clear that, when the average INP concentration λ is smaller than 1, i.e. on average less than one cell per droplet, there must be droplets devoid of any cells because the number of cells in an individual droplet can only be an integer (assuming only whole cells – without fragments – are present). In such a case, heterogeneous ice nucleation cannot be triggered in every droplet but only in those containing at least one cell. Hence, homogeneous ice nucleation is expected to occur in the empty droplets. Moreover, even if the average INP concentration λ is exactly one per droplet, there will be a few droplets that contain two or more INPs and, thus, other droplets that do not contain any INPs. The distribution of INPs among microfluidic droplets at small average INP concentration can be described using Poisson statistics (Huebner et al., 2007; Köster et al., 2008; Edd et al., 2009; Collins et al., 2015). The detailed documentation of this procedure is given in the Supplement.
2.4 Elemental analysis
The total carbon content of the F. cylindrus samples has been determined using elemental analysis. For this purpose, an amount of 0.7 mg F. cylindrus diatoms was combusted at a high temperature (T>1000 ∘C) in a tin crucible, and the composition was analysed using a commercially available elemental analyser (EuroVector, Euro EA Elemental Analyzer).
3.1 Ice nucleation of F. cylindrus
Initially, the ice nucleation activity of F. cylindrus diatom cells was studied by differential scanning calorimetry (DSC). We found that fragments or exudates of F. cylindrus diatoms are potential ice nucleators, as the sample containing F. cylindrus diatoms induces freezing. The results are described in detail in the Supplement and in Fig. S8. These experiments initiated a more detailed study using the WISDOM microfluidic device. First, we investigated the ice nucleating properties of samples containing F. cylindrus diatom cells, in addition to fragments and exudates, at different concentrations suspended in artificial seawater. We used the droplet microfluidic device described in Sect. 2.3.2 above. The results of these experiments are presented in Fig. 2a, which shows, as a function of temperature, the frozen fraction of droplets fice, commonly defined as the cumulative number of droplets frozen when cooled to a certain temperature relative to the total number of droplets (Murray et al., 2012). Thus, fice is practically independent of the total number of droplets investigated in a particular experiment. In our case, the number of droplets varied between 45 and 70 droplets per single measurement, and typically three single measurements per sample were performed. Figure 2a shows that the freezing temperatures of all F. cylindrus samples (coloured symbols) are higher than that of the artificial seawater reference sample (grey symbols), hence supporting the observations from the DSC experiments that the F. cylindrus diatoms promote ice nucleation. To compare the different samples, we use the T50 temperature, which is the temperature at which half of the observed droplets are frozen, i.e. fice=0.5. For the artificial seawater, we measured a T50 of −40.1 ∘C, and T50 of the F. cylindrus suspensions shifted to a higher temperature by between about 2.8 and 7.2 ∘C with increasing diatom concentration. Detailed information on the increase in T50 of the different concentrations is given in Table S4. This significant concentration dependence of the T50 shift reveals that not all diatoms nucleate ice at the same temperature, and this implies a distribution of the ice nucleation efficiency as has been observed previously also for other ice nucleators (Herbert et al., 2014; Budke and Koop, 2015).
This is visualized better by plotting the cumulative number nN of ice nucleating sites per number of F. cylindrus diatom cells, defined in Eq. (S9), as a function of freezing temperature (see Fig. 3). This nN value is independent of the concentration of investigated INP and of the size of the investigated droplets but can be measured for a wide range of temperatures, using different concentrations, and allows for the comparison with results from other experimental techniques (see the discussion below). Figure 3 reveals that, at −30.0 ∘C, ∼0.1 % of the F. cylindrus diatom cells promote ice nucleation, which increases to ∼1 % at −32.0 ∘C and ∼10 % at −33.5 ∘C. Between about −35.0 and −36.5 ∘C all F. cylindrus cells trigger the nucleation of ice, i.e. nN=1. By definition, nN values larger than 1 should not be possible because it would imply that one diatom can induce the freezing of more than one droplet, which is unreasonable. The highest nN values occur at the lowest diatom concentrations, and therefore, we must consider Poisson statistics, i.e. whether or not each droplet indeed contains a diatom cell. Following the treatise mentioned in Sect. 2.3.3 and outlined in detail in the Supplement and using Eq. (S7), in Fig. 3 we indicate all the droplets that contain at least one diatom as filled circles, while all droplets that do not contain any F. cylindrus diatom cells are displayed as open circles. This analysis reveals a relatively sharp transition between filled and unfilled circles at nN values of about one ice nucleating active site per diatom cell. All droplets frozen at nN1 (and lower temperatures) do not contain intact F. cylindrus cells. We suggest that their freezing is induced by cell fragments or by INPs released by the F. cylindrus diatoms, e.g. soluble species from the EPSs such as proteins or polysaccharides. A similar behaviour has been observed previously for birch pollen that releases about 104 ice nucleators per pollen particle, which turned out to be ice nucleating macromolecules (Pummer et al., 2012, 2015; Augustin et al., 2013; Dreischmeier et al., 2017).
To verify the above interpretation, we performed experiments in which the samples from the measurements shown in Figs. 2a and 3 were filtered with a pore size of 0.22 µm. This procedure removes intact whole diatoms, which are about 4.5 to 74 µm for the apical axis and 2.4 to 4 µm for the transapical axis (Lundholm and Hasle, 2008; Cefarelli et al., 2010). In Fig. 2b, the cumulative fraction of frozen droplets of these filtered samples is shown. The symbol colours represent the same suspensions as shown in Fig. 2a, but filtered, and the artificial seawater reference data are identical to that in Fig. 2a. All frozen fraction curves are shifted to lower temperatures when compared to the unfiltered samples, suggesting a significant, but not entire, removal of INPs. Only the filtrate of the suspension with the lowest concentrations reveals a T50 that is the same as the seawater reference (−40.1 ∘C), suggesting that this sample does not contain any significant concentration of INPs after filtration. All other filtrated suspensions show T50 values that are higher by between 2.6 and 6.4 ∘C relative to the seawater. For further information on the T50 shifts, see Table S4. Together, these results imply that either fragments of F. cylindrus or molecules released by the diatoms can nucleate ice but with a significantly reduced efficiency than intact diatoms. Moreover, these results can also explain the observations in Fig. 3 of ice nucleation of droplets at nN1 that do not contain any full diatom cells. Below, we present further experiments to investigate the nature of the ice-nucleating particles.
3.2 Ice nucleation of resuspended F. cylindrus cells
In the following experiments, we separated diatom cells from their fragments or released INPs. For this purpose, the sample suspension of F. cylindrus with a concentration of 1×107 cells per millilitre, which was shown already in Fig. 2, was analysed further, and the results are presented in Fig. 4. The green data points are those of the unfiltered sample, which is identical to that shown in Fig. 2a, and the magenta data points are identical to the filtered solution already presented in Fig. 2b (shown there as green data points). This suspension should contain only INPs smaller than 0.22 µm. Next, most (but not all) of the diatom cells and fragments contained in the filter cake of that filtration procedure were resuspended in artificial seawater. Thus, the concentration of the resuspended cells is about 2×106 cells per millilitre (estimated uncertainty range 1×106–1×107 cells per millilitre). The frozen fraction of that sample is shown as the orange data points in Fig. 4 and shows the same ice nucleation onset temperature of about −32.5 ∘C as the original unfiltered suspension (green). However, the curve is broader, suggesting that it contains less of the most active ice nucleators. To verify that all fragments smaller than 0.22 µm had been leached out during the first filtration step, this resuspended filter cake sample was filtered again with a 0.22 µm filter. The results of this procedure on the freezing behaviour are shown as the blue circles in Fig. 4. The frozen fraction data are practically identical to that of the artificial seawater, suggesting that the filtration of the pure whole cells has been successful, and hardly any fragments smaller than 0.22 µm are left in the filtrate. This analysis also implies that the ice nucleation of the unfiltered suspension is due to whole cells and cell fragments but not due to ice nucleating molecules released from the diatoms. The T50 shift upon filtration of about 1.5 ∘C is similar in magnitude to the effect of reducing the concentration of the unfiltered diatoms from 5×107 to 1×107 cells per millilitre, i.e. by a factor of 5. This similarity may indicate that fragments make up about 10 %–20 % of the INPs in the unfiltered samples, which agrees with the fact that some ice nucleation is observed for values of nN1 (see Fig. 3).
3.3 Ice nucleation of spent medium and of purified fcIBP11
We also investigated the spent medium (Guillard and Ryther, 1962), i.e. the medium in which the F. cylindrus diatoms were cultivated before they were separated by centrifugation to investigate their ice nucleating effects. Separation of the diatoms from the spent medium by centrifugation is not perfect, and hence, smaller fragments, in addition to soluble macromolecules such as proteins, may remain in the spent medium. These may be potential ice nucleators, as it has been shown previously that even smaller ice-binding antifreeze proteins can act as ice nucleators at lower temperatures (Eickhoff et al., 2019).
In Fig. 5 we compare the frozen fraction curve for the spent medium (light green circles) with that of a freshly prepared medium, which had never been in contact with any F. cylindrus diatoms (olive circles). Clearly, the spent medium, even after centrifuging off the diatoms, shows significant ice nucleation with a T50 of about −35.7 ∘C, while the T50 of the fresh medium is much lower at −40.0 ∘C. In additional experiments, the spent medium has been filtered in two further steps, first by using a 0.22 µm syringe filter (light blue circles) and then by using a 100 kDa centrifugation filter (pink circles). For comparison, the fresh medium has been also filtered with a 100 kDa centrifugation filter (purple circles). Obviously, filtration of the spent medium with a 0.22 µm filter shows hardly any effect on ice nucleation, as its T50 is shifted to −36.0 ∘C, which is the same as the unfiltered sample within the temperature uncertainty in our set-up of ±0.3 ∘C.
In contrast, filtration with a 100 kDa filter substantially reduced the ice nucleation with a T50 value of −40.6 ∘C, which is the same as that of the filtrated fresh medium of −40.7 ∘C, suggesting that the 100 kDa filter removed all remaining ice nucleators present in the spent medium. This observation suggests that any macromolecules smaller than 100 kDa that were present in the spent medium are not ice nucleation active because otherwise they would have passed the filter and led to an increased T50 when compared to the fresh medium. The ice-binding proteins present in and/or released from F. cylindrus are similar in size to the well-characterized fcIBP11, which is about 26 kDa (Bayer-Giraldi et al., 2011). Thus, ice-binding proteins released by the F. cylindrus into the spent medium should have passed the filter and could have induced ice nucleation if they had significant ice nucleation activity. However, the results shown in Fig. 5 do not reveal any ice nucleation activity. This may be interpreted as follows. Either the proteins remaining in the filtrate do not promote ice nucleation or F. cylindrus does not release any proteins into the spent medium. To shed further light on the ice nucleating ability of ice-binding proteins from F. cylindrus, we studied purified fcIBP11 samples in additional experiments. We studied the ice nucleation activity of two fcIBP11 solutions of different concentrations and that of the pure Tris-HCl buffer for comparison. The results are presented in Fig. 6. The two fcIBP11 samples with 0.1 mM (dark blue circles) and 0.01 mM (light blue circles) concentrations reveal T50 values of −39.8 and −39.4 ∘C, which are equal to the T50=39.7 ∘C of the buffer reference (black circles) within experimental temperature uncertainty (±0.3 ∘C). Thus, no significant shift in the freezing temperature is observed, and even when considering the increased ice nucleation temperature of the fcIBP11 at frozen fractions below about 25 %, it appears that fcIBP11 is not an efficient ice nucleator with relevance for atmospheric or biospheric processes, owing to its unnaturally high concentration in the droplet samples investigated here. These observations agree with recent theoretical studies, which suggest that moderate antifreeze IBPs show no nucleation of ice perpendicular to the basal and prismatic ice planes (Cui et al., 2022). And indeed, the basal and prismatic planes are exactly those planes at which the moderate fcIBP11 binds to ice (Kondo et al., 2018).
Overall, the results show that F. cylindrus diatom cells and cell fragments suspended in seawater can induce heterogeneous ice nucleation, while ice-binding proteins produced by F. cylindrus, such as fcIBP11, have negligible ice nucleation activity.
Here, we put the above results in the context of previous ice nucleation studies on diatoms. Triggered by the pioneering initial laboratory studies of marine-diatom-induced ice nucleation (Alpert et al., 2011; Knopf et al., 2011), modelling studies have shown that, in some regions of the atmosphere, marine diatoms may contribute to the atmospheric INP (Burrows et al., 2013; Ickes et al., 2020). To use laboratory ice nucleation data in such models, the data must be evaluated and parameterized appropriately. For example, a direct comparison of T50 or fice originating from different laboratory studies on different types of INPs is not meaningful, as different sample volumes, INP concentrations, buffer concentrations, etc., may have been used. Therefore, it is preferable to compare the cumulative number of ice nucleating active sites per mass, surface area, or the number of the INPs. Here, we make a comparison based on total INP mass, using the following definition of the cumulative number of ice nucleating active sites per mass nm_total (Murray et al., 2012; Hiranuma et al., 2015, 2019; Xi et al., 2021).
Here, V is the volume of an individual droplet in the experiment, and cm_total is the total mass of biological material per droplet. For the F. cylindrus samples investigated here, we used the total carbon mass per F. cylindrus cell from the literature (Kang and Fryxell, 1992) and performed elemental analysis to obtain the carbon content of our samples, resulting in a value of 39.32 % to calculate the average total mass per individual F. cylindrus diatom cell of g. Using these values and our experimental data in Eq. (1), we have calculated the ice nucleating active sites nm_total of the F. cylindrus diatoms (see the blue circles in Fig. 7). We have fitted this data set and provide a corresponding parameterization (see Fig. S9 and Eq. S10.) Also shown in Fig. 7 are nm_total data of the sea ice diatoms Melosira arctica (blue squares) and Nitzschia stellata (blue triangles) and of the temperate diatom Skeletonema marinoi (open orange circles) from previous studies (Ickes et al., 2020; Xi et al., 2021).
To allow a direct comparison of ice nucleation of the different diatoms, which were studied in different types of aqueous solutions, all the ice nucleation temperatures shown in Fig. 7 have been corrected (either by the original authors or by us) for the colligative solute effect and represent diatom ice nucleation in pure water. We have corrected the freezing temperatures of the F. cylindrus samples by the measured difference between the T50 of pure double-distilled water and pure artificial seawater without any diatoms.
The comparison in Fig. 7 reveals that the curves of the three sea ice diatoms complement one another, as nm_total values of different magnitudes have been obtained over different temperature ranges. Interestingly, while some offsets exist between the different data sets, their slopes are quite similar. In contrast, the slope of the nm_total data of the temperate diatom is significantly smaller. The observed similarities of the sea ice diatom data sets suggest a more generalized description of their behaviour in models. For this purpose, we fitted these data sets to provide a parametrization of nm_total as a function of temperature. The three different data sets consist of different numbers of data points which were taken into account in order to give each data set the same statistical weight. We further note that one strongly deviating data point from the M. arctica data set (indicated as an open square in Fig. 7) was excluded from the fitting procedure. The resulting parameterization is given as follows:
where T is temperature to be entered in units of degrees Celsius. For numerical code verification, Eq. (2) should result in a value for nm_total of 6.7×105 g−1 at a temperature of −20.0 ∘C. This parameterization is valid over the temperature range between −13.7 and −34.5 ∘C. The parameterization is shown as the thick solid line in Fig. 7, and the upper and lower 2σ prediction bands are given as dashed lines. In summary, Fig. 7 shows that the parameterization line and its prediction bands are an appropriate representation of the ice nucleation activity of three types of sea ice diatoms suitable for use in atmospheric or biogeosciences model applications.
In the following, we put the ice nucleation data of F. cylindrus and the other sea ice diatoms into context by comparing to field studies. Wilson et al. (2015) provided experimental evidence for a marine biogenic source of ice nucleating particles and suggested that exudates and fragments of diatoms as a source of the ice nucleating material located in the sea surface microlayer. Their low-temperature freezing data reveal a cumulative number of ice nucleating active sites per total organic carbon mass nm_TOC of g−1 at −27 ∘C (calculated from the equation given in the caption of their Fig. 2), which is the low-temperature end of their data, and the most relevant to the present study. To compare this value to the nm_total values given in Fig. 7, we estimated that the organic carbon content of their samples varies between 39.32 % (representing the organic carbon content of F. cylindrus cells; see above) or 100 % (representing a purely organic carbon composition), resulting in a range of nm_total of –1.3×1010 g−1 for their Arctic sea surface microlayer samples. These are compared to nm_total values of 8.2×107 g−1 (2σ prediction bands of 2.8×107–2.4×108 g−1) for F cylindrus and of 5.8×108 g−1 (2σ prediction bands of 7.0×107–4.8×109 g−1) for sea ice diatoms, respectively, at −27 ∘C, indicating that F. cylindrus and other sea ice diatoms may contribute to the marine INP in the Southern Ocean and Antarctic seawater, assuming the Wilson et al. (2015) parameterization also applies to these areas.
In another comparison, we use measurements of insoluble aerosol particles made at Amsterdam Island in the southern Indian Ocean (Gaudichet et al., 1989). These measurements show that marine biogenic particles make up between 8 % and 28 % of the number of detected particles and that these were predominantly assigned to Radiolaria and diatom fragments (identified as amorphous silicates), with about 27 % or 2.7×104 m−3 particles observed in the southern winter (July) and fewer in fall (May; 8 %; 2.4×104 m−3) and spring (September; 7 %; 1.8×103 m−3). If we assume that all Radiolaria and diatom fragments can be attributed to F. cylindrus diatoms, we can calculate the mass concentration of F. cylindrus diatom cells per cubic metre of air from the mass of an individual cell ( g; see above), yielding values of g m−3 of air (July), g m−3 of air (May), and g m−3 of air (September). Using the parametrization of the cumulative number of ice nucleating active sites per mass F. cylindrus in Eq. (S10), we calculate a nm_total value of 8.2×107 g−1 (2σ prediction bands are 2.8×107–2.4×108 g−1) at −27 ∘C (see above), from which we can derive the ∼88 INP m−3 air (2σ of 3–250) at −27 ∘C in fall (May). This value can be compared to in situ total INP measurements in the Southern Ocean south of Australia in fall (March–April), yielding values between 34 and 207 INPs per cubic metre of air at −27 ∘C (McCluskey et al., 2018). Although the above calculations are order-of-magnitude estimates, the comparison shows that it is not unreasonable that sea ice diatoms such as F. cylindrus, and their fragments may constitute a significant fraction of the INP in the Southern Ocean and Antarctic waters.
Cells and fragments of F. cylindrus diatoms can induce heterogeneous ice nucleation in artificial seawater by up to 7.2 ∘C higher temperature (for the largest concentration investigated, i.e. 5×107 cells per millilitre) than the homogeneous ice nucleation temperature in pure seawater. We also observed an ice nucleating effect of fragments smaller than 0.22 µm, in agreement with previous observations of the relevance of nanoscale biological fragments for ice nucleation (O'Sullivan et al., 2015; Wilson et al., 2015; Irish et al., 2017, 2019; Hartmann et al., 2021). For the ice-binding (antifreeze) protein fcIBP11, we did not observe any evidence for promoting ice nucleation at low temperatures. Using the information that F. cylindrus may serve as INPs, we can estimate their atmospheric relevance. Due to their smaller size and, thus, longer atmospheric residence time, especially fragments of diatoms are expected to be relevant for atmospheric ice nucleation because the atmospheric lifetime of entire F. cylindrus diatoms is estimated to be below 1 d due to deposition (Hobbs, 2000; Seinfeld and Pandis, 2016). There are only a few studies that describe the aerosolization and atmospheric transport processes of diatoms and diatom fragments in addition to their atmospheric detection at different altitudes (Brown et al., 1964; Gaudichet et al., 1989; Leck and Bigg, 2008; Burrows et al., 2013). Based on order-of-magnitude estimations comparing field observations of the Southern Ocean with our laboratory results, we suggest that diatoms like F. cylindrus and their fragments may contribute to ice nucleation in marine environments of the polar regions at low temperatures where sea ice diatoms become active for ice nucleation (Fig. 7). To improve these estimates, more observations of the atmospheric abundance of diatoms and INPs in general and in the Antarctic marine environments are required, and modelling studies of the sea-to-air transfer of diatoms and their fragments are needed. In this respect, we observed a common behaviour of the cumulative number of ice nucleating active sites per mass of diatom among three different types of sea ice diatoms. This similarity may originate from a similar biological function of the ice nucleation ability in sea ice diatoms, and a corresponding parameterization developed thereof may simplify the representation of their properties in atmospheric and biogeochemical models.
The experimental data presented in the figures of this paper are provided in tabular form in the Supplement.
The supplement related to this article is available online at: https://doi.org/10.5194/bg-20-1-2023-supplement.
LE and TK designed the study. MBG provided the protein samples, LE performed the calibration and both DSC and microfluidic ice nucleation experiments, and NR prepared the microfluidic devices. LE did the data analysis and the Poisson statistics calculations, with input from TK. LE and TK prepared the figures. LE, TK and MBG wrote the paper, with input from YR and NR. All authors contributed to the discussion of the data and text and approved the final version of the paper.
The contact author has declared that none of the authors has any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We thank Arika Allhusen and Klaus Valentin, for providing the original F. cylindrus samples, and Luisa Ickes, Yu Xi, and Allan Bertram, for provision of original data sets on diatom ice nucleation and for helpful comments.
We acknowledge support for the publication costs by the open-access publication fund of Bielefeld University and the Deutsche Forschungsgemeinschaft (DFG). Maddalena Bayer-Giraldi is grateful for support from the Deutsche Forschungsgemeinschaft SPP1158 (German Research Association programme no 1158; grant no. BA 3694/2-1). This open-access publication was funded by Bielefeld University.
This paper was edited by Anja Engel and reviewed by Manuel Dall'Osto and one anonymous referee.
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