The impact of (bio-)organic substances on the ice nucleation activity of the K-feldspar microcline in aqueous solutions
- Department of Environmental Systems Science, Institute for Atmospheric and Climate Sciences, ETH Zurich, 8092 Zurich, Switzerland
Correspondence: Kristian Klumpp (firstname.lastname@example.org) and Claudia Marcolli (email@example.com)
Potassium feldspars (K-feldspars), such as microcline, are considered key dust minerals inciting ice nucleation in mixed-phase clouds. Besides the high ice nucleation activity of microcline, recent studies also revealed a high sensitivity of microcline to interaction with solutes on its surface. Here, we investigate the effect of organic and bio-organic substances on the ice nucleation activity of microcline, with the aim to better understand the underlying surface interactions. We performed immersion freezing experiments with microcline in solutions of three carboxylic acids, five amino acids, and two polyols to represent these compound classes. By means of a differential scanning calorimeter we investigated the freezing of emulsified droplets of microcline suspended in various solutions. Depending on the type of solute, different effects were observed. In the case of carboxylic acids (acetic, oxalic, and citric acid), the measured heterogeneous onset temperatures, Thet, showed no significant deviation from the behavior predicted by the water activity criterion, , which relates Thet with the melting point temperature Tmelt via a constant water activity offset Δaw. While this behavior could be interpreted as a lack of interaction of the solute molecules with the surface, the carboxylic acids caused the fraction of heterogeneously frozen water, Fhet(aw), to decrease by up to 40 % with increasing solute concentrations. In combination, unaltered Thet(aw) and reduced Fhet(aw) suggest that active sites were largely deactivated by the acid molecules, but amongst those remaining active are also the best sites with the highest Thet. A deviation from this behavior is citric acid, which showed not only a decrease in Fhet, but also a decrease in Thet of up to 4 K for water activities below 0.99, pointing to a depletion of the best active sites by interactions with the citrate ions. When neutralized solutions of the acids were used instead, the decrease in Fhet became even more pronounced. The slope of Thet(aw) was different for each of the neutralized acid solutions. In the case of amino acid solutions, we found a decrease in Thet (up to 10 K), significantly below the Δaw criterion, as well as a reduction in Fhet (up to 60 %). Finally, in the case of the investigated polyols, no significant deviation of Thet from the Δaw criterion was observed, and no significant deviation of Fhet in comparison to a pure water suspension was found. Furthermore, we measured the effects of aging on the ice nucleation activity in experiments with microcline suspended in solutions for up to 7 d, and tested the reversibility of the interaction with the solutes after aging for 10 d. For citric acid, an ongoing irreversible degradation of the ice nucleation activity was observed, whereas the amino acids showed completely reversible effects. In summary, our experiments demonstrate a remarkable sensitivity of microcline ice nucleation activity to surface interactions with various solutes, underscoring the importance of the history of such particles from the source to frozen cloud droplets in the atmosphere.
The formation of ice has various implications for key characteristics of clouds. The presence of ice significantly influences cloud lifetime, the formation of precipitation, cloud chemistry, and radiative properties (Lohmann, 2006; Field and Heymsfield, 2015; Mülmenstädt et al., 2015; IPCC, 2013). Numerous aspects of ice formation within clouds are still unclear, necessitating further research to elucidate the different ice nucleation mechanisms.
Ice formation takes place via homogenous or heterogeneous ice nucleation in supercooled cloud droplets. Homogeneous nucleation occurs spontaneously as a stochastic process when micrometer-sized pure liquid water droplets supercool to 235–238 K (Sassen and Dodd, 1987; Heymsfield and Sabin, 1989) and can be described by classical nucleation theory (e.g., Lohmann et al., 2016; Ickes et al., 2015). In aqueous solutions, the thermodynamic formulation by Koop et al. (2000) describes the homogeneous freezing point curve as a function of water activity, aw, of the solution, i.e., the ratio between the water vapor pressure of the solution and of pure water under the same conditions:
This relationship is termed the “water activity criterion” or the “Δaw criterion for homogeneous ice nucleation”, which states that, owing to the thermodynamic properties of water and irrespective of the nature of the solute, the homogeneous freezing point curve can be constructed from the melting point curve, Tmelt, by a constant water activity shift Δaw,hom (Koop and Zobrist, 2009). This approach has a broad empirical basis and theoretical underpinning (Baker and Baker, 2004). In contrast, heterogeneous ice nucleation is induced by solid particles present in the water or solution, so-called ice-nucleating particles (INPs). More specifically, the nucleation takes place on active sites, which are preferred locations for ice nucleation (IN) with areas of 10–50 nm2 based on estimates from classical nucleation theory (Vali, 2014; Vali et al., 2015; Kaufmann et al., 2017; Holden et al., 2019). Depending on the circumstances of ice nucleation, different modes of IN are possible: (i) immersion freezing describes the freezing process when an INP is immersed in a supercooled droplet. (ii) Condensation freezing is assumed to occur when IN coincides with cloud droplet activation (Vali et al., 2015; Kanji et al., 2017). (iii) Contact freezing may occur when nucleation is initiated by an INP that penetrates the droplet surface, e.g., through a collision (Durant and Shaw, 2005; Shaw et al., 2005; Nagare et al., 2016). (iv) Finally, deposition nucleation is the term for a freezing process happening without the liquid water phase involved and therefore assuming a direct transition of gaseous water to ice on an INP surface. The latter is currently questioned by Marcolli (2014), who suggested water vapor condensation in pores with subsequent pore water freezing (termed pore condensation and freezing, PCF) to be the dominant nucleation process at water-subsaturated atmospheric conditions.
Since the introduction of the Δaw criterion by Koop et al. (2000) for homogeneous freezing, numerous studies found that Δaw= const. might under certain circumstances also be applicable to heterogeneous nucleation in immersion freezing mode occurring in the presence of solutes (Zobrist et al., 2008a; Knopf and Alpert, 2013; Koop and Zobrist, 2009; Rigg et al., 2013), albeit with . The relation Δaw,het = const. suggests that the freezing point depression is merely determined by the influence of the solute on aw, whereas specific interactions between the solutes and the INP surface are absent.
Among the particles that are considered important as atmospheric INPs, mineral dust particles are the best-established particle type. The ability of mineral dust particles to nucleate ice depends on their mineralogical composition. Among the minerals present in transported dust (Reid et al., 2003; Murray et al., 2012; Boose et al., 2016), quartz, feldspars, and clay minerals such as kaolinite, montmorillonite, and illite have been found to be IN-active (Hoose and Möhler, 2012; Pinti et al., 2012; Hiranuma et al., 2015a; Kumar et al., 2019a, b; Harrison et al., 2019), while other frequent minerals like calcite, dolomite, and micas exhibit negligible IN activity (Kaufmann et al., 2016; Kumar et al., 2019b). Atkinson et al. (2013) emphasized the exceptionally high IN efficiency of K-feldspars compared to other minerals. Indeed, several studies confirmed that K-feldspars nucleate ice at higher temperatures with higher activated fractions than (Na–Ca) feldspars (Peckhaus et al., 2016; Kumar et al., 2018; Kaufmann et al., 2016; Harrison et al., 2016). But also within the group of K-feldspars, IN activities differ, with microcline being IN-active at higher temperatures than orthoclase, adularia, and sanidine (Kaufmann et al., 2016; Welti et al., 2019). Despite the high proportion of feldspars in the Earth's crust, they make up only 13 % of the airborne dust aerosol by mass (Murray et al., 2012). However, considering that particles above 1 µm in diameter are typically aggregates of different minerals, even minor contributions of microcline can determine the IN characteristics of a particle.
Yet, ice nucleation by mineral dust, which mostly nucleates ice below 255 K (Murray et al., 2012; Atkinson et al., 2013; Kaufmann et al., 2016; Boose et al., 2016), fails to explain the occurrence of ice in clouds at even higher temperatures. Therefore, in recent years, biological particles gained attention as INPs because of their ability to nucleate ice well above 255 K (Hoose et al., 2010; DeMott and Prenni, 2010; Conen et al., 2011; Pummer et al., 2012; O'Sullivan et al., 2014, 2015; Twohy et al., 2016; Stopelli et al., 2017; Cascajo-Castresana et al.,2020; Huang et al., 2021). Biological particles are of a very diverse nature and include bacteria, pollen, spores, and fragments of plants and animals (Murray et al., 2012; Morris et al., 2013; Després et al., 2012; Kanji et al., 2017). The IN-active entities can be traced back to macromolecules that include polysaccharides (Steinke et al., 2020) and cellulose (Hiranuma et al., 2015b, 2019), lignin (Bogler and Borduas-Dedekind, 2020; Steinke et al., 2020), humic or fulvic substances (Fornea et al., 2009; Wang and Knopf, 2011; Borduas-Dedekind et al., 2019), and proteinaceous material (Huang et al., 2021). Among these macromolecules, IN activity strongly varies. The ice-active proteins expressed by Pseudomonas syringae may nucleate ice up to 271 K, but only when they are arranged on the outer cell membrane of the intact cell (Maki et al., 1974; Schnell and Vali, 1976; Govindarajan and Lindow, 1988). Freezing at similarly high temperatures has also been observed for related bacterial species and some fungi, most probably also originating from proteinaceous nucleation sites (Lindow et al., 1978; Kim et al., 1987). Yet, even proteins that are not expressed for the purpose of nucleating ice, such as the iron-storing protein apoferritin, have proven to be ice-active up to 269 K when clustered together in aggregates (Cascajo-Castresana et al., 2020). Peat soil, fulvic acids, and aquatic dissolved organic matter showed average freezing temperatures between 260 and 265 K (Fornea et al., 2009; Borduas-Dedekind et al., 2019). Ice nucleation by cellulose only becomes relevant at 252 K (Hiranuma et al., 2015b; 2019), although freezing onsets may reach as high as 269 K. For lignin, freezing onsets were observed below 263 K with a 50 % frozen fraction reached only at 254 K (Bogler and Borduas-Dedekind, 2020).
Biogenic material is inferred to increase the ice nucleation ability of soil dust compared with desert dust based on various studies showing that the IN activity of collected soil dust samples decreases when the samples are treated with heat or hydrogen peroxide to remove (bio-)organic residues from the dust samples (Conen et al., 2011; Tobo et al., 2014; O'Sullivan et al., 2018; Paramonov et al., 2018). Similarly, glacial outwash sediments exhibited high IN activity, most probably stemming from the presence of small amounts of biogenic material, since treatment with hydrogen peroxide reduced the IN-active site densities to values found for illite NX (Tobo et al., 2019), which is often taken as a proxy for mineral dust (Hiranuma et al., 2015a). However, the treatment of bulk samples with heat or hydrogen peroxide does not provide insights into whether synergistic effects between (bio-)organic substances and mineral dust particles are involved in the high IN activity of soil dust. Such effects have been suggested by O'Sullivan et al. (2014) as their soil dust samples froze at higher temperatures than either humic-like substances (HULIS) or mineral dust references by themselves. Only a few studies have investigated the mixing state of mineral dust and biogenic material and its relevance for the IN activity. Pratt et al. (2009) found external mixtures of mineral dust and biological particles using aircraft aerosol time-of-flight spectrometry applied to cloud ice-crystal residues, yet they were IN-active only at quite low temperatures (239–242 K). Conversely, single-particle analysis of agricultural harvesting emissions also revealed, besides pure dust and biological particles, a considerable fraction of dust particles mixed with organic or biological material (Suski et al., 2018). Finally, O'Sullivan et al. (2016) found that ice-nucleating proteins from Fusarium avenaceum, a common soil-borne fungus, preferentially bind to kaolinite and impart their ice-nucleating properties to it.
Instead of already adhering to mineral dust particles before entering the atmosphere, organic and biological material may also attach to the mineral particle surface during cotransport in the atmosphere by coagulation with organic particles or condensation of semivolatile organic molecules. The influence of such coatings may depend on various factors such as the thickness and chemical composition of the coating, affecting the nature of the interaction. Recent investigations showed that mineral dust surfaces are sensitive to exposure to inorganic solutes, leading to deviation from const. Whether the solutes enhance or deteriorate the IN activity compared with const. depends on the mineralogy of the particles, the nature and concentration of the solutes, and the freezing temperature range. Figure 1 provides a schematic overview of the different interactions between solutes and the mineral dust surface in aqueous solutions, which include ion exchange, adsorption, and dissolution of the mineral surface. Panel (a) depicts the case with no specific interactions between the solute and the mineral surface such that const. is fulfilled. Cation exchange, as depicted in panel (b), may occur for minerals with exchangeable cations and has been shown to decrease the IN activity of feldspars in general (Kumar et al., 2018, 2019b; Whale et al., 2018; Perkins et al., 2020; Yun et al., 2020). Ammonia and ammonium salts have been proven to generally increase the IN activity of aluminosilicates, which includes feldspars and clay minerals, most probably through both ion exchange (panel b) and adsorption (panel c). In the case of quartz, enhancing and deteriorating interactions of the solutes with the surface seem to compete as the presence of ammonia decreased the freezing onset temperatures due to dissolution (panel d) of the mineral surface in basic solution, while the presence of ammonium sulfate has a slight enhancing effect, probably due to adsorption (Kumar et al., 2019a; Whale et al., 2018). The effect of dissolution depends on the dissolution process, which again depends on the specific mineral. In the case of microcline, dissolution is accompanied by the formation of an amorphous silica layer as explained in Kumar et al. (2019b). There is increasing evidence that ice nucleation does not occur on the whole mineral surface but on specific nucleation sites, which are often considered to be defects. Since defects are less stable than the regular mineral surface, we expect them to dissolve first, thus enhancing the effect of dissolution on IN activity.
To extend these findings, we aim to gain insight into possible interactions between mineral surfaces and (bio-)organic solutes. We chose microcline to provide the mineral surface as this feldspar showed, on one hand, high IN activity, while, on the other hand, it proved to be highly sensitive to the presence of solutes. The organic solutes were selected to represent typical functional groups present in organic and proteinaceous materials. The hydroxyl groups of polyols feature the prevailing functional group of polysaccharides and cellulose and are also frequent in lignin, fulvic, and humic acids. We chose glycerol and 1,7-heptanediol to represent these types of organics. To represent the carboxyl groups of fulvic and humic acids, we chose a monovalent (acetic acid), a bivalent (oxalic acid), and a trivalent organic acid (citric acid). The number of carboxyl groups in an organic acid influences the complexation of Al3+ present in feldspars, in turn modulating the ability of the organic acid to interact with the mineral surface. Moreover, as the strongest carboxylic acid, oxalic acid is supposed to have the most pronounced effect on feldspar dissolution because of its acidity, which was shown to deteriorate the IN activity of microcline in the presence of H2SO4 (Kumar et al., 2018). Finally, with amino acids, we test how interactions between the microcline surface and the building blocks of proteins influence the IN activity. In solution, amino acids are present as zwitterions with carrying the negative and the positive charge (see Fig. A1 in the Appendix). Both groups have the potential to interact with the microcline surface. The similarity of to and NH3 raises the question of whether such interactions may enhance the IN activity of feldspars. We chose glycine, l-alanine, l-serine, l-lysine, and l-glutamine to cover relevant functionalities found in proteins (see Table 1 for structures and properties). Glycine, as the simplest amino acid, provides the basic case of no additional functionalities in the side chain. l-Alanine possesses an aliphatic tail as the side chain, providing the case without the possibility for polar interactions. With a hydroxyl side chain, serine is capable of additional polar interactions. l-Lysine and l-glutamine possess longer side chains with additional amino and amide functional groups, respectively, that may interact with the microcline surface. With the amino group, l-lysine has an additional basic group, increasing the pH of the solution to the basic range. Furthermore, all selected amino acids are sufficiently water-soluble to potentially modify the microcline surface distinctly. Besides representing functionalities found in biogenic material, the investigated organic acids are oxidation products of a lot of organic substances, polyols are intermediate products before further oxidation yields carboxylic acids, and amino acids were detected in the atmosphere in various locations (Barbaro et al., 2011, 2015).
1 Calculated using the weak acid approximation: pH = 0.5⋅(pKa−log 10(cacid)) (cacid, mol L−1). 2 Calculated using the semi-strong approximation and consideration of the first two acidic protons: (cacid, mol L−1). .
Using a differential scanning calorimeter (DSC) setup, we will present results from immersion freezing experiments of microcline suspensions dispersed as emulsified solution droplets.
2.1 Particle size distribution and surface area of the microcline powder sample
For the experiments described herein, two stones of microcline were used, both from North Macedonia provided by the Institute of Geochemistry and Petrology of ETH Zurich. Both stones were milled with a tungsten carbide disk mill, resulting in a fine powder. The first stone is identical to the one used by Kumar et al. (2018). The second stone was milled in October 2019 following the same protocol as for the first stone. X-ray diffraction followed by Rietveld analysis of powder samples yielded the following composition: (86.33 ± 1.7) % microcline, (6.18 ± 0.72) % orthoclase, and (7.49 ± 0.48) % albite for the first sample and (91.9 ± 0.8) % microcline and (8.9 ± 0.4) % albite for the second sample. The number size distributions of the mineral dust particles suspended in water were measured using laser diffraction analysis (see the Supplement).
The specific surface area was determined using dynamic vapor sorption (DVS) analysis, yielding a value of 1.6 m2 g−1 for the first and 3.1 m2 g−1 for the second sample.
2.2 Immersion freezing experiments of emulsified microcline suspensions in water and aqueous solutions
Immersion freezing experiments were conducted with a differential scanning calorimeter (DSC) Q10 from TA instruments (see Zobrist et al., 2008a, for more details). Suspensions of microcline (2 wt %) in aqueous (molecular bioreagent water, Sigma-Aldrich) solutions containing different organic acids, amino acids, and polyols as detailed in Table 1 were prepared. In order to prevent particle aggregation, all samples were sonicated 5 to 10 min before experiments were started. After sonication the suspensions were combined with a mixture of mineral oil (95 %) and lanolin (5 %) (both Sigma-Aldrich) at a ratio of 1:4 and emulsified with a rotor stator homogenizer (Polytron PT 1300D with a PT-DA 1307/2EC dispersing aggregate) for 40 s at 7000 rpm for the measurements including the organic acids, the neutralized organic acids, and the polyols (Sect. 3.1.1, 3.1.2, and 3.3). For all other measurements the procedure was readjusted to 40 s dispersing at 10000 rpm using a lanolin content of 7 % to obtain a droplet size distribution that peaks at 2–3 µm with respect to number and 4–12 µm with respect to volume (for more details see Marcolli et al., 2007; Pinti et al., 2012; Kaufmann et al., 2016). This readjustment was required after the rotor stator had broken and was replaced by a new one of the same model (Polytron PT 1300D with a PT-DA 1307/2EC dispersing aggregate). Occasionally, single large droplets may form, which appear as spikes in the thermogram upon freezing. These spikes were neglected in the evaluation. 5 to 10 mg of the emulsion was placed in an aluminum pan, hermetically sealed, placed in the DSC, and measured at cooling and heating rates of 1 K min−1. To test the stability of the emulsion, some samples were subjected to three freezing cycles following the procedure introduced by Marcolli et al. (2007) with a first and third cycle performed with a cooling rate of 10 K min−1 as control cycles. Emulsions were freshly prepared before each experiment. Every experiment was repeated at least once with a freshly prepared suspension unless stated otherwise (see figures and figure captions). For evaluation of the freezing onset temperatures (Thet and Thom), the heterogeneously frozen fraction (Fhet), and the melting temperature Tmelt, freezing and cooling cycles run at 1 K min−1 were used.
Figure 2 shows a typical DSC thermogram of an aqueous microcline emulsion. Depicted is the heat flow of the sample as a function of temperature. Freezing events are accompanied with a release of latent heat, resulting in a peak in the thermogram. The first peak at higher temperatures arises from heterogeneous freezing caused by microcline in the emulsion droplets. The second peak is due to the homogeneous freezing of the remaining droplets, which either contain no microcline particles or whose microcline particles lack active sites. Our key parameters to analyze the thermograms are the onset temperatures of these peaks, Thet and Thom, together with the heterogeneously frozen fraction (Fhet). We quantify Fhet by taking the integral over the portion of the thermogram between Thet and Thom as shown in Fig. 2. The heat released during freezing is approximately proportional to the volume of water that freezes in the sample with a minor deviation from this proportionality arising from the temperature dependence of the freezing enthalpy (Speedy, 1987; Johari et al., 1994). Table 2 provides a summary of the uncertainty in each parameter. We consider a decrease or increase in Fhet to be a loss or gain of IN-active surface area. Assuming freezing on nucleation sites (Vali et al., 2015), this corresponds to the loss or generation of such sites. Conversely, a change in quality of the IN-active surface area due to the deterioration or improvement of nucleation sites would lead to a decrease or increase in Thet. A concomitant decrease in Fhet is expected if some sites deteriorated to an extent that they cannot compete with homogeneous ice nucleation anymore. Since Thet and Fhet are not able to capture the exact form of the heterogeneous freezing curve, we provide all DSC thermograms in the Supplement. To derive the water activity from the melting point depression, the melting temperature (Tmelt) is evaluated at the maximum of the melting peak. See Fig. 2 for a detailed description of the evaluation of Thet, Thom, and Fhet.
2.3 Neutralization of carboxylic acid solutions with ammonia
In order to discriminate between the influence of the carboxylate anion and the cation (H+ providing acidity to the solution) of the dissociated carboxylic acids on microcline, suspensions were prepared with neutralized solutions of acetic acid, oxalic acid, and citric acid. Acid solutions were neutralized by adding aqueous ammonia (25 % (aq), Merck) solution until a pH of 6–8 was reached (tested by pH test strips, Macherey-Nagel). For neutralization we deliberately chose ammonia solution and no other alkaline substance because the influence of ammonia on microcline has been well characterized by Kumar et al. (2018).
2.4 Immersion freezing experiments as a function of aging
Microcline suspensions in citric acid (1 wt %), l-alanine (1 wt %), and l-lysine (0.05 wt %) solutions were prepared (see Table 1 for information on supplier and purity) and investigated by DSC over the course of 7 d to test the long-term influence of the solutes on the microcline surface. Measurements were performed directly after preparation and on the first, fourth, and seventh day after preparation. The suspensions were sonicated 5 min prior to each measurement in order to resuspend settled particles and to decrease particle aggregation.
2.5 Reversibility of interactions between microcline and solutes tested in immersion freezing experiments
Microcline suspensions in citric acid (10 wt %), l-alanine (10 wt %), and l-lysine (2 wt %) solutions were prepared and aged in a sealed glass vial at room temperature for 10 d. After aging, all suspensions were centrifuged (3 min at 600 rpm), the supernatant was removed, and the remaining sample washed with water. This procedure was repeated five times. The washed particles were resuspended in water. Finally, immersion freezing experiments were conducted with these suspensions to compare the freezing properties of the aged microcline dust with freshly prepared suspensions in water.
3.1 Carboxylic acids
3.1.1 Freshly prepared carboxylic acid samples
Figure 3 shows the melting temperatures (Tmelt) and homogeneous and heterogeneous freezing onset temperatures (Thom and Thet) as a function of water activity (aw) for microcline (2 wt %) in aqueous acetic, oxalic, and citric acid solutions. Analogous to the procedure described in Kumar et al. (2018), water activities were determined from the melting temperatures obtained from the DSC thermograms using the parameterization introduced in Koop et al. (2000). Therefore, the plotted melting temperatures perfectly align on the ice melting curve (dash-dotted line). Furthermore, we assume the water activities at the freezing temperatures to be identical to those determined at the melting temperature. This approximation may lead to errors, since water activities show a dependence on temperature, which may explain some of the deviations of the measured homogeneous freezing points from the homogeneous freezing curve (dotted line). Note that these temperature dependencies differ depending on the solute and are often small (Zobrist et al., 2008b; Ganbavale et al., 2014). The homogeneous and heterogeneous freezing curves (black solid and dotted lines, respectively) were obtained by constant shifts in water activity, Δaw,hom and Δaw,het, applied to the ice melting curve (Koop et al., 2000; Zobrist et al., 2008a). Both Δaw,hom and Δaw,het were calculated to match the average onset temperatures of all measurements performed with the two pure microcline samples (2 wt %) at a water activity of aw=1, which yielded and a heterogeneous offset . Note that Δaw,hom is slightly lower than the values 0.305 and 0.313 determined by Koop et al. (2000) and Koop and Zobrist (2009), respectively, in order to take the characteristics of our DSC experiment (droplet size distribution and uncertainty in temperature calibration) into account. The solid black curve represents the heterogeneous freezing onset temperature expected in the absence of specific interactions between the ice-nucleation-active surface and the solute, i.e., , assuming that Thet is given solely by the freezing point depression due to the decreased water activity as depicted in Fig. 1a.
For the experiments with the freshly prepared carboxylic acids and the neutralized acid suspensions the first sample was used. For this sample, Thet and Fhet of 2 wt % microcline in pure water are 251.7 K and 0.69, respectively, while it was 251.4 K and 0.81 for the second sample, which was used for the aging and recovery experiments as well as the measurements with the amino acids. The values measured for pure microcline sample 1 in this study are slightly lower than those found by Kumar et al. (2018; Thet=251.9 K/ Fhet=0.75), while the second sample yields slightly higher values in Fhet and slightly lower values in Thet.
Figure 3a shows that the heterogeneous freezing temperatures of microcline in aqueous acetic and oxalic acid solutions fulfill at all measured concentrations within experimental uncertainty. Citric acid shows a deviation towards lower temperatures of up to 4 K for aw<0.99, i.e., const. The carboxylic acids investigated here show neither the clear enhancement of ammonia-containing solutes nor the clear decrease in inorganic “non-ammonia” solutes, which were found by Kumar et al. (2018). However, the heterogeneous freezing curve of all carboxylic acids broadens and the median freezing temperature shifts to lower temperature (see Figs. S1–S3), which is manifested in a decrease in Fhet as shown in Fig. 3b and points to a loss of IN activity in acid solution (high H+ concentration). The same was observed by Kumar et al. (2018) for microcline in sulfuric acid solutions and by Yun et al. (2021) in carboxylic and inorganic acid (HNO3 and HCl) solutions with a trend of decreasing IN activity with decreasing pH (Yun et al., 2021). For acetic acid, as the weakest acid, the decrease in Fhet is indeed the least and levels off after a first decline.
3.1.2 Neutralized carboxylic acid samples
To test the hypothesis that high concentrations of H+ (low pH) cause the loss of microcline IN activity, we neutralized the carboxylic acid solutions with ammonia to a pH of 6 to 8. We chose ammonia as the neutralizing base, as Kumar et al. (2018) have shown that ammonia does not deteriorate the ice nucleation activity of microcline. On the contrary, it can even enhance it.
Figure 4 shows the results of these experiments, i.e., the melting (Tmelt) and freezing onset temperatures (Thet, Thom) of microcline in all three aqueous dicarboxylic acid solutions neutralized to pH 6–8 with ammonia. Similarly to the ammoniated solutions investigated by Kumar et al. (2018), an increase in Thet is observed for water activities close to 1 and a decrease for lower water activities. For citric and oxalic acid, the enhancement is restricted to a very narrow concentration range (1>aw>0.99) and reverts to a clear decline for higher concentrations that exceeds the one observed in the respective pure acid solutions shown in Fig. 3. None of the neutralized carboxylic acids satisfy the Δaw criterion, i.e., , and all of them behave differently from one another. Similarly to the pure acids and in clear contrast to ammonia, the neutralized acid solutions show a strong decrease in Fhet towards lower water activities, which is the strongest for oxalic acid, followed by citric acid, and the least for acetic acid. This dependence on the specific neutralized acid suggests the presence of interactions between the carboxylic acid or the carboxylate anions and the microcline surface.
The differences between the tested carboxylates can be explained by the complexation of Al3+ with the deprotonated carboxylic acids. Indeed, bidental and tridental carboxylic anions have the potential to complex aluminum, while the ability of monodental carboxylates was found to be negligible (Stoessell and Pittman, 1990). Several studies have shown the ability of oxalate to complex Al3+ (Bevan and Savage, 1989; Stoessell and Pittman, 1990; Min et al., 2015). With three acid groups, citric acid might be a similar or even stronger complexing agent. Conversely, adsorption of acetic acid is weaker, as it carries only one carboxylic acid group. This explains why the trend of Thet (see Fig. 4a) for microcline in neutralized ammonium acetate solutions (blue squares) is similar to the one for ammonia solutions (cyan diamonds), since ammonia or the ammonium ion dominates surface interactions with respect to acetate. Yet, based on experiments with freshly prepared microcline suspensions, it remains unclear whether carboxylate complexation leads to enhanced dissolution of microcline or whether it blocks IN-active sites of microcline through adsorption of the carboxylic anions on the mineral surface.
3.1.3 Aging experiments
In order to detect changes occurring during aging within atmospherically relevant timescales, we performed experiments in which microcline (2 wt %) was immersed in the solutions over the course of 7 d (Fig. 5) with measurements on days 1, 4, and 7. Figure 5a shows no significant change in Thet and Fhet over 7 d when microcline is suspended in pure water, yet inspection of the thermograms reveals a shift of the median freezing temperature by about 1.4 K to lower temperature for the aged samples. For the same type of experiment with a different microcline sample, Kumar et al. (2018) observed a decrease in Fhet by one-third after 1 d but no drop in Thet. Conversely, Peckhaus et al. (2016) found a decrease of 2 K in the median freezing temperature after 5 months for their microcline sample. These differences in IN activity after aging highlight differences between microcline samples, which may be explained by minor contributions from other minerals that differ from sample to sample and differences in microtexture (Whale et al., 2017).
Figure 5b shows the DSC thermograms of microcline aged in citric acid solution (1 wt %, aw≈0.995). They evidence a further decrease in Fhet and Thet starting on day 4. There is also a visible change in the shape of the thermogram (the maximum of the heterogeneous freezing peak shifts to lower temperatures). This shows that surface modifications are ongoing, leading to progressive loss of IN activity over time. Figure 6 (light green curve) shows the thermogram after 10 d of aging in 10 wt % citric acid solution (aw≈0.984) and subsequent washing with pure water. The heterogeneous freezing peak of microcline after this procedure has almost completely disappeared. This illustrates the irreversibility of the surface modification induced through citric acid after 10 d.
The decrease in Fhet with decreasing aw, the continuous activity loss over time, and the irreversibility suggest that there is a permanent destruction of active sites, which was also shown by Kumar et al. (2018) for sulfuric acid acting on microcline. As carboxylic and sulfuric acid both release H+ to the solution, we conclude that high H+ concentrations (low pH) lead to the irreversible loss of ice-active sites of microcline through dissolution as depicted in Fig. 1d.
Figure 5c shows DSC thermograms of microcline suspended in neutralized citric acid solution (1 wt %; aw≈0.993). At this concentration, the IN activity of freshly prepared microcline even exceeds the curve of const., which we ascribe to the presence of ammonia. Contrary to the aging in a citric acid solution the IN activity remained stable over the observed time period, supporting the hypothesis that high H+ concentrations are the cause for the permanent loss of ice-active surface sites through dissolution. This is reinforced by Fig. 6 (dark green curve), which shows that even if aged in a higher concentration of neutralized citric acid (10 wt %; aw≈0.975), the IN activity is restored after washing and resuspension of the sample in pure water. This reversibility indicates that the strong decrease in IN activity during exposure (Fig. 4; Thet=235.9 K and Fhet = 0.16) to neutralized acid solutions is caused by blocking of IN-active sites through surface complexation rather than loss of active sites through dissolution (adsorption mechanism in Fig. 1c). The blocking scenario is in agreement with findings by Bevan and Savage (1989), who showed that suspending K-feldspars in neutralized oxalate solutions increases surface dissolution only weakly compared with strongly increased dissolution rates induced by high H+ concentration. The heterogeneous freezing onset temperature of microcline in neutralized citric acid solution is even higher than in pure water, most likely caused by small amounts of ammonia that are still present in the sample, since ammonia already has an enhancing effect on IN activity of microcline at very low concentrations (Kumar et al., 2018).
Figure 7 shows melting (Tmelt) and freezing onset temperatures (Thet, Thom) of microcline in aqueous glycerol and 1,7-heptanediol solutions. Over the whole measured concentration range, both solutes show full compliance with . Similarly, no significant deviation of Fhet compared to the pure microcline sample was observed. This suggests that the interaction of these molecules with the ice-nucleating sites on the microcline surface must be very similar to the ones of water molecules, namely a fast dynamic exchange of molecules at the microcline surface corresponding to the case shown in Fig. 1a. As a result, neither an enrichment nor a depletion of the polyol molecules occurs on the microcline surface. In consequence, these molecules affect the IN activity only via the reduction of the water activity to the extent predicted by the Δaw criterion. These findings are in accordance with Yun et al. (2021), who found no significant effect of polyols on the median freezing temperature of potassium-rich feldspar.
3.3 Amino acids
3.3.1 freshly prepared amino acid samples
Figure 8 shows melting (Tmelt) and onset freezing temperatures (Thet, Thom) of microcline in aqueous solutions of glycine, l-alanine, l-serine, l-lysine, and l-glutamine. All five tested amino acids show a clear and relatively uniform decrease in Thet(aw) of up to 9.1 K below . Similarly to the carboxylic acids and the neutralized carboxylic acids, Fhet strongly decreases with decreasing water activity for l-lysine, while the other amino acids show only a moderate decrease in Fhet.
3.3.2 Aging experiments
Figure 9 shows the DSC thermograms of microcline suspended in solutions of l-alanine (1 wt %; aw≈0.994) and l-lysine (0.05 wt %; aw≈0.9985) over the course of 7 d, measured on days 1, 4 and 7. We chose l-lysine because it showed the strongest decrease in the fresh measurements and l-alanine as a representative of the other amino acids. The amino-acid-containing suspensions show more variability in Fhet and Thet over the course of 7 d compared to the pure microcline sample but no clear tendency during the observed time span. Furthermore, Fig. 10 (magenta and orange curves) shows that after the procedure of 10 d aging in more concentrated solutions (l-alanine 10 wt %, aw≈0.977; l-lysine 2 wt %; aw≈0.993) and subsequent washing, the thermograms show no significant difference from the pure microcline sample after the same procedure. Despite the strong response observed in the freezing experiments in freshly prepared suspensions, the aging experiments show that ice nucleation is directly affected by the presence of the amino acids with no additional aging effect. This indicates that the interaction of the amino acids with the microcline surface is reversible once the solutions are removed or highly diluted. This fits the adsorption mechanism depicted in Fig. 1c. Due to the zwitterionic properties of the amino acids (Fig. A1) the positively charged functional groups can establish very stable interactions with the negatively charged microcline surface, which explains the strong response of Thet. This may also explain the relatively strong reaction of l-lysine (also in Fhet) because with its additional amino group, it is able to form an additional positively charged functional group by receiving H+ from the surrounding water. Contrary to the case of ammonia, this strong adsorption goes along with a decrease in IN activity, since the amino acids – in contrast to ammonia – do not exhibit positively polarized H atoms ready for hydrogen bonding to the water oxygen.
Depending on the solute, different influences on the freezing onset temperatures and the heterogeneously frozen fraction were observable. Overall, these investigations confirm the high sensitivity of the IN activity of microcline to solutes, as was already shown for inorganic salts (Kumar et al., 2018; Whale et al. 2018; Yun et al., 2020) and sulfuric acid (Kumar et al., 2018).
The carboxylic acids investigated here and the sulfuric acid investigated by Kumar et al. (2018) show similar effects on the IN activity of microcline, namely Thet following the Δaw criterion and Fhet decreasing with increasing concentration, together with irreversibility of the decrease. This supports the conclusion that the effect of acids originates primarily from the surface interaction with H+, leading to dissolution and only secondarily from interactions with the anions. The influence of anions becomes visible in experiments under neutral pH, evidencing the complexation of Al3+ in the surface layers of the mineral. Bidentate complexes of oxalate (and dicarboxylic acids in general) with Al3+ have been reported to accelerate the dissolution of the feldspar anorthite, which is the Ca2+ end-member of the plagioclase series (Min et al., 2015). Yet, because the higher Si : Al ratio of microcline (3:1) compared with anorthite (1:1) leads to a higher number of Si–O–Al compared with Al–O–Al bonds (Oelkers and Schott, 1995; Oelkers et al., 2009), dissolution is much lower in microcline because the aluminum ions are more tightly bound within the crystal lattice through Si–O–Al bonds compared with Al–O–Al bonds. A slight effect of carboxylic anions on the dissolution of feldspars has been shown by Bevan and Savage (1989), who independently varied pH and oxalic acid concentrations in K-feldspar suspensions and found strongly enhanced surface dissolution when pH was decreased compared with only a small increase in dissolution when the oxalate concentration was increased. We therefore conclude that, on the timescales of our experiments, bidentate and tridentate carboxylates decrease the IN activity by blocking active sites through surface adsorption rather than by dissolving them. Surface complexation is smaller for acetic acid since, as a monocarboxylic acid, it cannot form bidentate complexes with Al3+. We also speculate that complexation with carboxylic acids would decrease the IN activity of microcline irreversibly on longer timescales. We assume that in the case of feldspars with a lower Si-to-Al ratio, surface complexation would immediately promote dissolution. Under strongly acidic conditions (pH 1), Bevan and Savage (1989) found decreased dissolution rates of K-feldspar in the presence of oxalic acid. This indicates that H+-catalyzed dissolution can even be inhibited instead of promoted by oxalate complexation. Yet, at such high H+ concentrations, dissolution dominates complexation by far, leading to a net loss of active sites within the timescale of our experiments.
The investigated amino acids show a decrease in Thet and Fhet, which is strongest in the case of l-lysine. Due to the zwitterionic nature of amino acids a strong polar interaction with the hydroxyl groups on the mineral surface is possible. Periodic density functional theory calculations have shown that glycine, the simplest amino acid, can interact with up to three surface silanol groups of microcline (Hu et al., 2020). The resulting adsorption of the molecules alters the surface properties and therefore influences the IN activity. In the case of l-lysine the additional, positively charged group is expected to additionally enhance the adsorption on the negatively charged surface of microcline (pHPZC<2; Vidyadhar and Hanumantha Rao, 2007), resulting in even lower Fhet. Hedges and Hare (1987) showed in experiments that basic (positively charged) amino acids adsorbed much better on clay mineral surfaces than neutral and acidic amino acids, confirming a dependence of surface adsorption on the surface charge of the mineral.
A reversible decrease in IN activity has also been observed by Zolles et al. (2015) after treating a microcline sample with papain and pronase E enzymes. The IN activity was restored after heating the enzyme-treated sample to 773 K. As enzymes consist of folded amino acid chains, the reduced IN activity of microcline in the presence of these proteins might be traced back to the blocking of nucleation sites through surface-adsorbed enzymes.
The effect of polyols on IN activity aligns with the Δaw criterion, which is in accordance with Yun et al. (2021) and findings from numerous studies that investigated the impact of organic coatings on various types of mineral dust (Tobo et al., 2012; Wex et al., 2014, for kaolinite + levoglucosan; Zobrist et al., 2008a; Koop and Zobrist, 2009, for ATD + polyethylene glycol). Kanji et al. (2019) investigated collected dust particles from the Sahara and Asia coated with secondary organic aerosol (SOA) from dark ozonolysis of α-pinene. The particles were coated, and subsequently the ice nucleation properties were observed in continuous flow diffusion chambers. Even though the SOA coating also contained carboxylic acid functional groups, no decrease in the IN activity of the dust was found in this study. However, as the share of microcline in the samples was not stated, the presence of other IN-active mineral components that do not respond as sensitively to organic acids as microcline may offer an alternative explanation for this finding. Apart from that, the H+ concentration and the competition of H+ with other complexing agents present in SOA also play a role in how accessible the mineral surface is for H+ ions of coated particles.
None of the(bio-)organic substances presented here enhanced the IN activity of microcline, which rules them out as a cause for enhanced IN activity of soil dust. Furthermore, interactions between the mineral surface and the most prevalent organic functional groups of the organic aerosol fraction leave the IN activity unchanged or even decrease it. These findings cast doubt on the conception that molecular interactions of organic molecules with the mineral surface may explain the enhanced IN activity of soil dust, and they leave ammonia and ammonium as the only identified agents that are able to increase the IN activity of mineral particles. Actually, ammonia is an omnipresent fertilizer of soils that indeed might have a share in increasing the IN activity of soil dust. In addition, ammonia will be removed by heating or H2O2 treatment, which are often used to infer the presence of (bio-)organic components (Du et al., 2017; O'Sullivan et al., 2014; Hill et al., 2016); this makes it an interfering agent in those tests.
Alternatively, or additionally, mineral particles may act as a substrate to order macromolecules such as humic acids, proteins, or fragments of even larger systems, thus enhancing their IN activity. In this case, the macromolecules would provide the active sites, which may be ordered to form larger IN-active structures on the mineral surface that are able to nucleate ice at higher temperatures. Such an effect due to aggregation on a substrate has been observed in the case of Pseudomonas syringae, for which the intact outer cell membrane provides a substrate for ordering the IN-active proteins into larger aggregates, thus raising the freezing temperatures by about 5 K (Polen et al., 2016; Zachariassen and Kristiansen, 2000). Findings of O'Sullivan et al. (2016) have shown that the IN activity of ice-nucleating proteins released from Fusarium avenaceum is conferrable to kaolinite dust particles when the protein encounters the mineral, yet without enhancing its IN activity. Thus, it remains an open question whether synergistic effects between (bio-)organic substances and mineral surfaces are able to enhance the IN activity of either component. Alternatively, biogenic macromolecules like proteins exhibit high freezing temperatures by themselves, and their presence alone may explain the increased IN activity of soil dust compared with bare mineral dust. This hypothesis also gains relevance considering that proteins not expressed for the purpose of nucleating ice can act as INPs (Cascajo-Castresana et al., 2020) at high temperatures (up to 269 K).
The high sensitivity to the presence of solutes gives rise to the question about the atmospheric relevance of microcline as an INP. Indeed, any investigated solute deteriorated the IN activity of microcline at water activities below 0.95. This is true for salts containing Na+, K+, and NH as cations, NO, SO, and Cl− as anions, and even more for acidic solutions (Kumar et al., 2018; Whale et al., 2018; Yun et al., 2020, 2021). Moreover, amino acids and neutralized dicarboxylic acids also deteriorated the IN activity as shown in this study. This has consequences for the relevance of coated microcline particles as INPs at cirrus conditions. Even if the coating inhibits ice nucleation reversibly, IN activity would only be restored at RH >95 %, which is well above the RH at which homogeneous ice nucleation in solution droplets sets in. Therefore, only uncoated microcline would be relevant as an INP at cirrus conditions. Conversely, microcline particles might act as INPs in immersion mode even when they are coated if the coating inhibited ice nucleation reversibly, which is the case for salts and amino acids, but not for acidic coatings or coatings with dicarboxylic acids. While mineral dust is uncoated at the source, it may obtain a coating during transport (Usher et al., 2003; Kolb et al., 2010; Ma et al., 2012; He et al., 2014; Fitzgerald et al., 2015; Tang et al., 2016). Even before long-range transport, soil dust contains organic material, which may inhibit ice nucleation of microcline if present as coatings on the particles. To establish the role of coatings in the IN activity of microcline, soil dust and aged airborne dust would need to be collected, analyzed with respect to its mineralogical composition, and investigated in controlled ice nucleation experiments.
Immersion freezing experiments with suspended microcline particles in different carboxylic acid, amino acid, and polyol solutions showed diverse effects on the IN activity of microcline attributable to their different surface interaction. The two investigated polyols showed agreement (within uncertainty) with the Δaw criterion and no significant change in the heterogeneously frozen fraction Fhet. The three examined carboxylic acids were also in agreement with the Δaw criterion, except for citric acid concentrations that correspond to aw<0.99. Yet, all three carboxylic acids cause a significant decrease in Fhet. When the acids were neutralized with ammonia, the decrease in Fhet was even more pronounced and the three acids yielded trends in Thet different from one another and from the Δaw criterion. The five amino acids showed decreased onset temperatures by up to 10 K below the Δaw criterion and decreased Fhet values. Furthermore, aging experiments showed that citric acid led to irreversible loss of ice-active sites, while aging in neutralized citric acid, l-lysine, and l-alanine solutions was completely reversible. This illustrates the different interactions of these solutes with the microcline surface. While acid solutions lead to irreversible loss of IN activity through dissolution of the microcline surface, the effect of all other investigated species is reversible and can be explained by adsorption, leading only to temporary loss of IN activity of microcline. Our investigations show that the IN activity of microcline is highly sensitive to bio-organic solutes, in agreement with other studies that showed a generally high sensitivity of microcline with respect to solutes. These findings highlight the need to investigate not only the IN activity of pure minerals but to extend these studies to investigations in the presence of species the minerals are in contact with throughout their emission and transport in the atmosphere. Furthermore, we cannot explain elevated IN activity of soil dust based on surface interaction of microcline with the bio-organics presented here.
The data presented in this publication are available at the following repository: https://doi.org/10.3929/ethz-b-000530486 (Klumpp, 2022).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-22-3655-2022-supplement.
KK conducted the experiments. KK, CM, and TP contributed to the planning and interpretation of the experiments. KK prepared the paper with contributions from CM and TP.
The contact author has declared that neither they nor their co-authors have any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We thank Michael Plötze, Anette Röthlisberger, and Marion Rothaupt for XRD and BET measurements; Philippe Grönquist and Christoper Dreimol providing us with DVS measurements; Marco Griepentrog for milling; Peter Brack for providing the microcline samples; and Ulrich Krieger, Uwe Weers, Nikou Hamzehpour, and Marco Vecellio for support in the laboratory (all ETH). We thank Silvan von Arx from the Institute of Mechanical Engineering and Energy Technology (Lucerne School of Engineering and Architecture, Lucerne) for providing size distribution measurements (laser diffraction particle sizer). We also thank Allan Bertram, Anand Kumar, and Jingwei Yun (Department of Chemistry, University of British Columbia, Vancouver) for a fruitful discussion.
This research has been supported by the Swiss National Foundation (project number 200021_175716).
This paper was edited by Ryan Sullivan and reviewed by two anonymous referees.
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