Article | Open

# Evidence of a reduction in cloud condensation nuclei activity of water-soluble aerosols caused by biogenic emissions in a cool-temperate forest

• Scientific Reports 7, Article number: 8452 (2017)
• doi:10.1038/s41598-017-08112-9
• Download Citation
Received:
Accepted:
Published online:

## Abstract

Biogenic organic aerosols can affect cloud condensation nuclei (CCN) properties, and subsequently impact climate change. Large uncertainties exist in how the difference in the types of terrestrial biogenic sources and the abundance of organics relative to sulfate affect CCN properties. For the submicron water-soluble aerosols collected for two years in a cool-temperate forest in northern Japan, we show that the hygroscopicity parameter κCCN (0.44 ± 0.07) exhibited a distinct seasonal trend with a minimum in autumn (κCCN = 0.32–0.37); these κCCN values were generally larger than that of ambient particles, including water-insoluble fractions. The temporal variability of κCCN was controlled by the water-soluble organic matter (WSOM)-to-sulfate ratio (R2 > 0.60), where the significant reduction of κCCN in autumn was linked to the increased WSOM/sulfate ratio. Positive matrix factorization analysis indicates that α-pinene-derived secondary organic aerosol (SOA) substantially contributed to the WSOM mass (~75%) in autumn, the majority of which was attributable to emissions from litter/soil microbial activity near the forest floor. These findings suggest that WSOM, most likely α-pinene SOA, originated from the forest floor can significantly suppress the aerosol CCN activity in cool-temperate forests, which have implications for predicting climate effects by changes in biogenic emissions in future.

## Introduction

Atmospheric aerosols play a key role in the climate system as they act as cloud condensation nuclei (CCN), and impact cloud formation1. The major factors controlling the activation of CCN include particle solubility and hygroscopicity, which are functions of chemical composition2, 3. The hygroscopicity parameter κ describes the influence of chemical composition on the CCN activity of aerosol particles4. Sulfate aerosol is one of the most effective components of CCN5 with κ values of greater than 0.6, whereas organics generally have lower κ values6, typically below 0.3 for biogenic secondary organic aerosols (BSOAs), for example. In forested regions with strong influence of biogenic sources, organic matter (OM) accounts for substantial fractions of the submicron particle mass. A majority of biogenic OM in submicron particles consists of BSOA derived from biogenic volatile organic compounds (BVOCs) including isoprene and monoterpenes, whereas primary biological aerosol particles (PBAPs) can also be a significant source of organic aerosol (OA). Because a large fraction of this biogenic OA is water-soluble7, the formation and abundance of biogenic OA relative to sulfate can modify CCN activity when organics coat sulfate particles. This type of coating can change the surface composition and water affinity of the particle.

Previous field studies conducted in areas dominated by biogenic OA, such as the Amazon8, 9, boreal forests10,11,12 or mountainous forests13, 14, have reported κ values below 0.3. Some studies have reported higher hygroscopicity for particles with larger diameters between 0.1 and 2.5 µm, which can be explained by the enrichment of sulfate in those particle size ranges9, 14, 15. Meanwhile, lower κ values for particles with diameters between 10 and 100 nm have been attributed to a larger fraction of organic mass9, 14, 15. Because most of the κ measurements were made by intensive field campaigns for periods of a few weeks, it is worth investigating how κ changes relative to changes in biogenic emissions throughout the year. Seasonal variability in CCN concentrations and aerosol hygroscopicity has been previously investigated in forested areas11,12,13, 16, 17, although limited chemical data is available to fully interpret them. Several field studies have shown lower hygroscopicity for particles in the accumulation mode in summer, which has been attributed to a large fraction of organic mass, likely of biogenic origin11, 13.

The objective of our research is to elucidate the impact of seasonal changes in the types and relative amounts of BSOA and PBAPs on the cloud forming potential of aerosols in forest environments. Submicron aerosol samples were collected in the Tomakomai Experimental Forest (TOEF) in northern Japan, which is a cool-temperate mixed forest. In this study, we show the impact of seasonal changes in the WSOM composition on the cloud forming potential of submicron aerosols by using molecular tracers with positive matrix factorization (PMF) analysis18. We also present evidence for modification of the aerosol hygroscopicity by specific types of biogenic emissions and discuss their implications for climate.

## Results and Discussion

### Seasonal variations in aerosol hygroscopicity

Figure 1 shows the seasonal variations in the monthly-averaged κCCN values of the submicron water-soluble aerosols in 2013 and 2015. The κCCN values ranged between 0.26 and 0.56 with an overall average of 0.44 ± 0.07. These κCCN values are generally larger than those for ambient particles obtained by in-situ measurements in other forest environments (typically below 0.3)8,9,10,11,12,13,14,15,16. This is expected, given that the aerosol from filter extracts is completely water-soluble, as well as because the observed aerosols at this study site were not purely organics, as discussed below. The κCCN values exhibited maxima in summer (June–August) and minima in autumn (September–November). This seasonal trend in κCCN was observed in both 2013 and 2015. The κCCN values in summer (0.50–0.52) are close to typical values of hygroscopic sulfate aerosols (~0.6). In contrast, the lower values observed in autumn (0.32–0.37) are similar to those for particles dominated by organics in forest environments, which typically range from 0.1 to 0.48,9,10,11,12,13,14,15,16.

While the seasonal pattern of κ is highly dependent on the location, Sihto et al.12 reported the lowest hygroscopicity in boreal forest in November, which they explained to be the result of a change in the chemical composition of aerosols. Paramonov et al.11 showed a seasonal variation in κCCN with a minimum (~0.2) in July and a maximum (0.74) in February with in-situ ambient measurements during a 29-month period in a boreal forest in southern Finland. Levin et al.13 also observed minimum κCCN values of 0.16 in July and September, and a maximum of 0.3 in April. Those previous studies suggested that the low hygroscopicity in summer was due to a larger organic mass fraction, which is likely attributed to increased emissions of BVOCs and subsequent formation of SOA. However, they have limited chemical measurements available to confirm this, although they mentioned that a change in the chemical composition of aerosols potentially affects κ. Because κCCN is closely linked to the chemical characteristics of aerosol4, our observations together with the previous studies in the forested areas suggest that a seasonal difference in the chemical composition could control the seasonal variation in κCCN.

### Seasonal trends of water-soluble organics and sulfate in submicron aerosols

In order to investigate the chemical composition of the observed submicron particles, Fig. 2a–b present seasonal changes in the mass fractions of water-extracted aerosols together with the mass concentrations of water-soluble organic carbon (WSOC) and sulfate in 2013. On average, sulfate was the dominant component in summer, accounting for ~59% of the submicron water-soluble aerosols. In contrast, the mass fractions (~35%) and concentrations of WSOM (WSOC) showed maxima in autumn (Table 1). These seasonal patterns were also observed in the year 2015 (Supplementary material, Table S1). Figure 3 displays the relationship between κCCN and the WSOM-to-sulfate ratios. Throughout the entire period of 2013, the κCCN value is negatively correlated with the WSOM/sulfate ratios (R2 = 0.60 and 0.66 for all the individual data and monthly average data, respectively). The R2 values were also as large as 0.79 (all data) and 0.76 (monthly averages) for the data obtained in 2015. This suggests that the fraction of organics relative to sulfate is an important factor that controls the CCN activity of the submicron water-soluble aerosols at the study site.

It should be noted that even during periods with similar WSOM-to-sulfate mass ratios of 0.62–0.64, κCCN differed between autumn (0.41–0.42) and winter (0.44–0.47) (Fig. 3), which indicates that the difference in the chemical composition of WSOM can modify κCCN. Specifically, it is suggested that WSOM in autumn contains less hygroscopic compounds than during the winter period. To explore the possible sources of WSOM and the resulting chemical compositions, Fig. 2c–f present the seasonal variations in the concentrations of representative tracers for BSOA and PBAPs. It is apparent that the concentrations of pinic acid, which is a first-generation oxidation product of α-pinene and is typically used as a tracer for α-pinene derived SOA19, 20, reach a maximum in autumn (Fig. 2c). Moreover, the concentrations of arabitol, trehalose, and mannitol also exhibited maxima during the same season (Fig. 2e), although the appearance of their peaks is slightly different from that of pinic acid. These sugar compounds are used as tracers of biological materials, including fungi and bacteria21, 22. In particular, trehalose is known to be a fungal metabolite as well as a stress protectant for the soil microbial community, and has been proposed as a molecular marker for fugitive dust from biologically active surface soils23. The seasonal profiles indicate that the increase of WSOM during the autumn period can be associated with increased concentrations of both α-pinene derived SOA and PBAPs.

Previous studies have suggested that α-pinene has been found to originate from roots, litter, and soil microbial activity24,25,26 in combination with high nitrification rates27. Local wind speeds were relatively low average 3.2 ± 0.5 m s−1 with a prevailing northerly wind (Supplementary material, Fig. S1) from the forested area in autumn. This supports the hypothesis of a significant influence of local emissions and subsequent vertical transport of α-pinene and its oxidation products within the canopy. Moreover, the enhanced concentrations of pinic acid together with these sugar compounds in autumn indicate that most of the observed pinic acid, and thus its precursor (α-pinene), in this season originated from the forest floor rather than from the leaves.

The concentrations of 2-methyltetrols, which is used as a tracer for isoprene-derived SOA28, showed a maximum in summer when the sulfate fraction dominated as described above. The seasonal trend of 2-methyltetrols (Fig. 2d) closely followed that of the ambient temperature (Table 1). The increased sulfate concentration is likely due to the higher influence of anthropogenic emissions originating from the industrial area of the Tomakomai city located in the south of the forest site. This is supported by the predominant southerly wind direction in summer (Supplementary material, Fig. S1).

### Source apportionment of WSOC by positive matrix factorization (PMF) analysis

We performed a PMF analysis to apportion sources of the measured WSOC, which is closely linked to κCCN. The PMF resolved five interpretable factors, which were characterized by the enrichment of each tracer compound (Supplementary material, Fig. S2). Factor 1 (F1) was dominated by the contribution of sucrose (89%), which is a primary saccharide of pollen grains. Consequently, it is referred to here as “pollen-rich”. Factor 2 (F2) is characterized by 2-methyltetrols (86%), whereas Factor 3 (F3) was dominated by pinic acid (75%). On the basis of the characteristics of each source profile, F2 and F3 are referred to here as “isoprene-SOA-rich” and “less oxidized α-pinene-SOA-rich”, respectively. Factor 4 (F4) is characterized by large contributions of mannitol (75%), arabitol (74%), trehalose (60%), and 3-methyl-1,2,3-butanetricarboxylic acid (3-MBTCA) (61%). It has been recognized that 3-MBTCA is a highly oxidized compound of α-pinene29. Although F4 was difficult to convincingly attribute to a specific source, given the possibility that these tracers for PBAP are associated with re-suspended soil and associated biota and that 3-MBTCA is a highly oxidized product of α-pinene, F4 was labeled here as “mixtures of fungi, bacteria, and more oxidized α-pinene SOA”. On the other hand, Factor 5 (F5) is dominated by sulfate (57%), sodium (54%), and ammonium (51%). The observed sulfate is suggested to originate from anthropogenic activity rather than from sea salt, because of the negligible fraction of sea-salt sulfate (<2%) calculated from the concentrations of sodium (Table 1). Consequently, F5 is referred to here as “anthropogenic sulfate-rich” as a possible source category of WSOC.

Figure 4 displays seasonal differences in the contribution of each source factor to the WSOC mass resolved by the PMF. The results show that 98% of the measured WSOC mass concentration in 2013 was successfully reproduced by the PMF model. In autumn, 75% of the WSOC mass was attributable to the sum of F3 and F4, both of which are dominated by the contribution of α-pinene derived SOA and fungi/bacteria derived WSOC. The significant contribution of α-pinene derived SOA was also apparent in spring, when the sum of F3 and F4 accounted for 57% of WSOC mass on average. The pollen-rich factor (F1) contributed only a minor fraction of the submicron WSOC, even in spring and summer (<7%). In summer, the anthropogenic sulfate-rich factor (F5) contributed significantly to WSOC mass (~57%), whereas the contribution of α-pinene derived SOA and fungi/bacteria derived organics to the WSOC was smaller (~28%). The increased concentrations of sulfate can also facilitate the formation of highly oxidized, hydrophilic OA, which implies that the formation of highly oxidized organics could have been a major component of observed WSOC in summer. In contrast, the WSOC in winter was attributed to less oxidized α-pinene SOA and anthropogenic sulfate-rich factors, with the lowest average concentration through the year. The present result indicates that the relative abundance and contributions of different sources to the WSOC mass are important for controlling the variation of the CCN activity.

### Factors controlling the hygroscopicity parameter at the forest site

The modification of κCCN associated with the increased contributions of α-pinene SOA is supported by previous studies. Oxidation products of α-pinene are known to be surfactants and as such, when mixed with inorganic salts, they have been found to affect the surface tension of the solution30,31,32. In general, depression in the surface tension caused by surfactants lowers the Kelvin (surface tension) effects33, which leads to increasing CCN activity31, 33, 34. On the other hand, surfactants also affect the Raoult (water activity) effects, which can compensate the Kelvin effects30, 31, 35. In mixed particles, κ can be modelled as the volume weighted average of the constituent’ κ values, which is estimated based on volume-mixing rules4. The estimated κ (κmix) is defined as κmix = ∑ɛ i κ i , where ɛ i and κi are the volume fraction and the κ value of each constituent, respectively. When κmix is simply determined for two-component mixtures of WSOM and ammonium sulfate (Table 1 and also see the method section), the observed κCCN and predicted κmix values agreed to within 17%, which is consistent with previous studies8, 10, 32, 36. It is noted that the κCCN shown here is the apparent κ, which is sensitive to the assumption used in the calculations (equations (1) and (2)) and is different from intrinsic κ37. Padró et al.32 evaluated κ for water-extracted aerosols in Mexico City by assuming the surface tension of water and 15% suface tension from the contributions of organics. They demonstrated that when κCCN is calculated allowing for a 15% surface tension depression, surfactant characteristics of the water-soluble aerosol can result in a reduction in organic hygroscopicity.

The reduction in hygroscopicity can be explained with an increased fraction of surface active organic compounds30, 31, 35. While surfactants generally reduce the surface tension effect (Kelvin effect) of the droplet, which leads to increased CCN activity33, 34, subsequent phase partitioning and/or organic coating lead to an organic-rich phase on the surface of the droplet and inner aqueous phase. This process can compensate for the surface tension effect if the fraction of surfactants is large. The surfactants lower the Raoult (water activity) effects31, 35, which may result in a reduction in CCN activity30, 31, 35. In recent laboratory experiments, Renbaum-Wolff et al.38 demonstrated that internally mixed sulfate and SOA, enriched with the oxidation products of α-pinene, results in a particle with a liquid-liquid phase separation. Furthermore, they showed that phase partitioning occurs with a phase enriched with α-pinene secondary OM on the surface of the particle and the water-rich inner phase above 95% RH. This surface organic-rich phase can prevent particles from activating as CCN. This mechanism can partly explain the reduction of κCCN in autumn, when the mass fraction of WSOM, dominated by α-pinene derived SOA, was large relative to that of sulfate.

It is interesting to note that F3 has a significant contribution of nitrate (53%; Supplementary material, Fig. S2). In fact, the concentration of nitrate showed a positive correlation with that of pinic acid (R2 = 0.26) in autumn, whereas there was an insignificant correlation with benzoic acid (R2 = 0.04; data not shown in this paper), which is measured as a tracer of anthropogenic origin. These results, together with low local wind speeds and prevailing wind direction from the forest area (Supplementary material, Fig. S1), indicate that a substantial fraction of the NOx originated from soil27 in the forest rather than from anthropogenic sources, to form aerosol nitrate. Nitrate radicals in the atmosphere are known to have a high reactivity to α-pinene and can subsequently form α-pinene nitrates39. Recently, chamber experimental and modelling studies have shown that the addition of nitrate functional groups inhibit CCN activation by reducing its miscibility with water40, 41, which also supports the observed reduction in CCN activity for particles in the vicinity of a biogenic source area.

In summary, our measurements indicate that in cool-temperate forests, where isoprene emissions are relatively low, the formation of α-pinene-derived SOA associated with soil/litter mostly found near the forest floor, can significantly contribute to reducing the cloud forming potential of submicron particles. Additional field studies are needed to investigate the mechanism for organics from the forest floor reducing the CCN activity. Future work should include more sample sets from multiple forest sites and provide comprehensive in-situ measurements of size distribution, chemical compositions, and CCN concentrations to evaluate the relationships of these physicochemical characteristics. The present findings might have important implications, and demonstrate that the seasonal variation in κ controlled by different types of biogenic sources is significant and should be taken into account in similar forest environments. They are also important for predicting regional climate effects due to changes in types and amounts of biogenic emissions particularly in cool-temperate/boreal forests in the future.

## Methods

### Location and submicron aerosol sampling

Ambient submicron aerosol samples were collected in Hokkaido University’s 2715 ha Tomakomai Experimental Forest (TOEF) (42°43′N, 141°36′E) located in the southwestern part of Hokkaido, northern Japan in the cool-temperate zone. The southern boundary of the forest site faces Tomakomai city and its industrial port area towards the Pacific Ocean. The mixed cool temperate forest consists of mature and secondary deciduous forest, and manmade coniferous forest with various types of forest floor covers. Tree species include Mongolian oak (Quercus crispula), mono maple (Acer mono), Korean mountain ash (Sorbus alnifolia), Japanese linden (Tilia japonica) and the planted species Japanese larch (Larix leptolepsis), sakhalin fir (Abies sachalinensis), and sakhalin spruce (Picea glehnii)42. The soil consists of volcanogenic regosols, which are shallow and less weathered43. The meteorological data for the sampling site was obtained from the Japan Meteorological Agency (available at http://www.jma.go.jp/jma/index.html). The predominant local wind direction in autumn and winter was from the north, corresponding to the forested area (Supplementary material, Fig. S1). In contrast, fractions of air transported from the south (coastal urban area) were dominant in summer. The monthly averaged temperature ranged from −1.9 ± 2.9 °C (winter) to 18.2 ± 3.1 °C (summer) for the years 2013 and 2015.

Submicron aerosol samples were collected continuously using a high-volume air sampler (HVAS; Model 120SL, Kimoto Electric, Osaka, Japan) at an altitude of ~18 m above the forest floor at the research site. A cascade impactor (CI; Model TE-234, Tisch Environmental, Cleves, OH, USA) attached to the HVAS was used to collect size-segregated particles44 with a flow rate of 1130 L min−1. In this study, we only used analytical results obtained from the bottom stage of the impactor, which collected particles with aerodynamic diameter smaller than 0.95 μm. The sampling duration of each aerosol sample was approximately 1 week. The samples were collected on quartz fiber filters (25 cm  × 20 cm) from January to December in 2013, and from February to December in 2015. Quartz fiber filters were pre-combusted at 410 °C for 6 hours to remove any contaminants. Collected filters were individually stored in glass jars with a Teflon-lined screwed cap at −20 °C to limit chemical reactions on the filter and losses of volatile compounds. In total, 37 samples for 2013 and 15 samples for 2015 have been analyzed, with the focus on 2013 presented in this study.

### Hygroscopicity measurement and determination of κCCN

To measure the hygroscopic parameters of submicron water-soluble aerosols, a filter cut of 0.79 cm2 was extracted with 7 mL ultrapure water using an ultrasonic bath (5 min × 3 times). The extracts were filtered through a 0.22 µm pore syringe filter (Millex-GV, 0.22 μm, Millipore) to remove any insoluble particles with diameters larger than 0.22 µm. Polydisperse aerosols were generated by first atomizing the filter extracts and then drying them with two diffusion dryers (silica gel and molecular sieve) in series. After passing the impactor and bipolar charger of the electrostatic classifier (TSI Model 3080), particles with a specific dry mobility diameter (Ddry) were selected by a differential mobility analyzer (DMA, TSI Model 3081). The classified flow was then split into two parallel streams: one went into the condensation particle counter (CPC, TSI Model 3775) to measure the total concentration of condensation nuclei (NCN), whereas the other stream was channeled into a continuous-flow thermal-gradient diffusion chamber (CCN-100, Droplet Measurement Technologies) to measure the number concentration of CCN (NCCN)45. The flow rate into the CCN counter was 0.5 L min−1 with a sheath-to-sample flow ratio of 10.

In order to measure size-resolved CCN activity and growth kinetics, Scanning Mobility CCN Analysis (SMCA) was performed46. In short, the method involves scanning a dynamic mobility diameter ranging from 10.4 to 220.7 nm with the DMA over a time period of 255 s. The specific supersaturation (SS, 0.25% to 1.0%) in the CCN counter was kept constant during the scan. The CCN activity of the particles generated was characterized by the activation diameter (Dact) at the corresponding SS, where the Dact of CCN is defined as the Ddry at which NCCN reaches 50% of the total NCN at a certain SS47. Dact can be determined by expressing the ratio of NCCN to NCN with respect to Ddry and fitting the data to a sigmoid curve47. A multiple-charge correction was applied to the NCCN and NCN using the algorithm provided in Moore et al.46. The algorithm re-bins misclassified multiply charged particles into their actual size bins based on an equilibrium charge distribution.

The hygroscopicity parameter, κCCN, can be calculated for particles with Ddry at a certain SS as follows4:

$κ(SS, D dry )≈ 4 A 3 27 D dry 3 ln 2 SS C$
(1)
$A = 4 σ s / a M w R T ρ w$
(2)

where SSC represents the critical supersaturation for activation, ρw is the density of water, Mw is the molar mass of water, σs/a is the surface tension of the pure water–air interface (σs/a = 0.072 J m−2), R is the universal gas constant, and T is the absolute temperature (T = 298 K). Calibration was performed with ammonium sulfate before and after the measurements. The hygroscopicity data are presented in the Supplementary material (Tables S3 and S4).

### Chemical analysis of water-soluble aerosols

The term water-soluble aerosols in the present study is technically defined as particles sampled on the filter and extracted with ultrapure water followed by being filtered through the syringe filter44, 48. To determine the WSOC concentration of the PM1.0 filter samples, another filter cut of 3.14 cm2 was extracted with 20 mL ultrapure water using an ultrasonic bath for 15 min. The extracts were filtered through the same type of 0.22 µm pore syringe filter as described above, before being injected into a total organic carbon analyzer (Model TOC-LCHP, Shimadzu). The mass concentrations of WSOC were converted to those of water-soluble organic matter (WSOM) using a conversion factor of 1.849, 50.

Another portion of the filter (3.80 cm2) was extracted with dichloromethane/methanol to measure biogenic molecular tracers: 2-methyltetrols (the sum of 2-methylerythritol and 2-methylthreitol)28, pinic acid, 3-methyl-1,2,3-butanetricarboxylic acid (3-MBTCA)19, 20, 29, trehalose, arabitol, mannitol, and sucrose21, 22. The –COOH and –OH functional groups in the extracts were reacted with N,O-bis-(trimethylsilyl) trifluoroacetamide (BSTFA) to form trimethylsilyl (TMS) esters and TMS ethers, respectively. The TMS derivatives were then analyzed for the compounds listed above using a capillary gas chromatograph (GC7890, Agilent) coupled to a mass spectrometer (MSD5975C, Agilent). Additionally, another cut of the filter (3.14 cm2) was extracted with 10 mL of ultrapure water under ultrasonication to determine the concentration of major inorganic ions (NO3, SO42−, Na+, NH4+, K+). The same syringe filter type as described above was used, before the extract was injected into the ion chromatograph (Model 761 compact IC; Metrohm)51. The data for the chemical measurements are given in the Supplementary material (Tables S5 to S7).

### Positive matrix factorization (PMF)

Positive matrix factorization (PMF)18 is a multivariate factor analysis technique used to resolve the identities and contributions of unknown mixtures to the observed components. Observed species are expressed as the sum of contributions from a number of time-invariant source profiles (factors) and residuals that cannot be modeled. By minimizing the residual term, the solution that best reproduces the observations can be determined. Further details of the PMF model and its application can be found elsewhere18, 52.

Thirteen chemical components in thirty-seven sample sets were used as input data in the PMF model for the year 2013 (Supplementary material, Fig. S2). The analytical measurement uncertainties of each component were taken into account for the calculation. The calculation was performed with 100 runs. To maximize the amount of data, missing values were replaced with the median values of the species53. The data from species with a signal-to-noise (S/N) ratio equal to or less than 0.5 were excluded from the analysis. Moreover, the data of species with an S/N ratio equal to or less than 1.0 were labeled as “weak”. Based on the scaled residual analysis with ±3 standard deviations, NO3 and NH4+ were additionally labeled as “weak”. Uncertainties for these weak species are tripled54. To determine the best solution, three to seven factor solutions were calculated, which resulted in the selection of five factors as the best solutions.

The uncertainty of the PMF solution is estimated by displacement (DISP) analysis and bootstrapping (BS) analysis55. With DISP, each fitted element of the factor profile in the solution is “displaced” by predetermined error levels to determine changes, or swaps, in the factor profiles. No swaps occurred at the lowest level. With BS, multiple PMF solutions are generated by using a series of data sets that are resampled versions of the original data set. By comparing the factor contributions, each BS factor is mapped to a base factor of the original PMF solution. The threshold of the minimum correlation for mapping was 0.6, and 100 bootstrapping runs were carried out. All BS factors could be mapped, and only BS Factor 4 showed mapping to the base Factor below 100% (94%) (Supplementary material, Table S2). In this case, four of the BS runs were mapped to F1 instead of F4, likely due to the fact that both factors contain contributions of PBAP tracers.

### Estimation of the predicted κ values

The predicted hygroscopicity parameter (κmix) was calculated by applying a mixing rule4 to the aerosol chemical composition as follows:

$κ m i x = ε A S κ A S + ε o r g κ o r g$
(3)

where κAS and κorg are typical κ values for ammonium sulfate (~0.6)4, 8 and biogenic secondary organic aerosols (~0.1)8, 56, respectively. The εAS and εorg values are the volume fractions of ammonium sulfate and organics, respectively, which were calculated from the mass concentrations using the density of ammonium sulfate (ρAS = 1.77 g cm−3) and the assumed density of organics (ρorg = 1.4 g cm−3)10.

## Additional Information

Publisher's note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

## References

1. 1.

Intergovernmental Panel on Climate Change (IPCC). Climate Change 2013 - The Physical Science Basis, doi:10.1017/CBO9781107415324 (Cambridge University Press, 2014).

2. 2.

McFiggans, G. et al. The effect of physical and chemical aerosol properties on warm cloud droplet activation. Atmos. Chem. Phys. 6, 2593–2649 (2006).

3. 3.

Lee, S., Ghim, Y. S., Kim, S. W. & Yoon, S. C. Effect of biomass burning and regional background aerosols on CCN activity derived from airborne in-situ measurements. Atmos. Environ. 44, 5227–5236 (2010).

4. 4.

Petters, M. D. & Kreidenweis, S. M. A single parameter representation of hygroscopic growth and cloud condensation nucleus activity. Atmos. Chem. Phys. 7, 1961–1971 (2007).

5. 5.

Seinfeld, J. H. & Pandis, S. N. Atmospheric chemistry and physics: from air pollution to climate change (Wiley, Inc., 2006).

6. 6.

Sun, J. & Ariya, P. Atmospheric organic and bio-aerosols as cloud condensation nuclei (CCN): A review. Atmos. Environ. 40, 795–820 (2006).

7. 7.

Kanakidou, M. et al. Organic aerosol and global climate modelling: a review. Atmos. Chem. Phys. 5, 1053–1123 (2005).

8. 8.

Gunthe, S. S. et al. Cloud condensation nuclei in pristine tropical rainforest air of Amazonia: size-resolved measurements and modeling of atmospheric aerosol composition and CCN activity. Atmos. Chem. Phys. 9, 7551–7575 (2009).

9. 9.

Pöschl, U. et al. Rainforest Aerosols as Biogenic Nuclei of Clouds and Precipitation in the Amazon. Science (80-.). 329, 1513–1516 (2010).

10. 10.

Cerully, K. M. et al. Aerosol hygroscopicity and CCN activation kinetics in a boreal forest environment during the 2007 EUCAARI campaign. Atmos. Chem. Phys. 11, 12369–12386 (2011).

11. 11.

Paramonov, M. et al. The analysis of size-segregated cloud condensation nuclei counter (CCNC) data and its implications for cloud droplet activation. Atmos. Chem. Phys. 13, 10285–10301 (2013).

12. 12.

Sihto, S.-L. et al. Seasonal variation of CCN concentrations and aerosol activation properties in boreal forest. Atmos. Chem. Phys. 11, 13269–13285 (2011).

13. 13.

Levin, E. et al. An annual cycle of size-resolved aerosol hygroscopicity at a forested site in Colorado. J. Geophys. Res. 117, D06201 (2012).

14. 14.

Levin, E. J. T. et al. Size-resolved aerosol composition and its link to hygroscopicity at a forested site in Colorado. Atmos. Chem. Phys. 14, 2657–2667 (2014).

15. 15.

Whitehead, J. D. et al. Biogenic cloud nuclei in the central Amazon during the transition from wet to dry season. Atmos. Chem. Phys. 16, 9727–9743 (2016).

16. 16.

Fors, E. O. et al. Hygroscopic properties of the ambient aerosol in southern Sweden – a two year study. Atmos. Chem. Phys. 11, 8343–8361 (2011).

17. 17.

Holmgren, H. et al. Hygroscopic properties and mixing state of aerosol measured at the high-altitude site Puy de Dôme (1465 m a.s.l.), France. Atmos. Chem. Phys. 14, 9537–9554 (2014).

18. 18.

Paatero, P. & Tapper, U. Positive matrix factorization: A non-negative factor model with optimal utilization of error estimates of data values. Environmetrics 5, 111–126 (1994).

19. 19.

Yu, J., Cocker, D. R. III, Griffin, R. J., Flagan, R. C. & Seinfeld, J. H. Gas-Phase Ozone Oxidation of Monoterpenes: Gaseous and Particulate Products. J. Atmos. Chem. 34, 207–258 (1999).

20. 20.

Claeys, M. et al. Hydroxydicarboxylic Acids: Markers for Secondary Organic Aerosol from the Photooxidation of α-Pinene. Environ. Sci. Technol. 41, 1628–1634 (2007).

21. 21.

Simoneit, B. R. T. et al. Sugars - Dominant Water-Soluble Organic Compounds in Soils and Characterization as Tracers in Atmospheric Particulate Matter. Environ. Sci. Technol. 38, 5939–5949 (2004).

22. 22.

Elbert, W., Taylor, P. E., Andreae, M. O. & Pöschl, U. Contribution of fungi to primary biogenic aerosols in the atmosphere: wet and dry discharged spores, carbohydrates, and inorganic ions. Atmos. Chem. Phys. 7, 4569–4588 (2007).

23. 23.

Rogge, W. F., Medeiros, P. M. & Simoneit, B. R. T. Organic marker compounds in surface soils of crop fields from the San Joaquin Valley fugitive dust characterization study. Atmos. Environ. 41, 8183–8204 (2007).

24. 24.

Peñuelas, J. et al. Biogenic volatile emissions from the soil. Plant. Cell Environ. 37, 1866–1891 (2014).

25. 25.

Aaltonen, H. et al. Agricultural and Forest Meteorology Boreal pine forest floor biogenic volatile organic compound emissions peak in early summer and autumn. Agric. For. Meteorol. 151, 682–691 (2011).

26. 26.

Faiola, C. L. et al. SOA Formation Potential of Emissions from Soil and Leaf Litter (2014).

27. 27.

Kirikae, M., Shibata, H., Tanaka, Y., Sakuma, T. & Hatano, R. Significance of nitrification and vegetation uptake in proton budgets in forest surface soil. Soil Sci. Plant Nutr. 47, 253–264 (2001).

28. 28.

Claeys, M. Formation of Secondary Organic Aerosols Through Photooxidation of Isoprene. Science (80-.). 303, 1173–1176 (2004).

29. 29.

Szmigielski, R. et al. 3-methyl-1,2,3-butanetricarboxylic acid: An atmospheric tracer for terpene secondary organic aerosol. Geophys. Res. Lett. 34, L24811 (2007).

30. 30.

Frosch, M., Prisle, N. L., Bilde, M., Varga, Z. & Kiss, G. Joint effect of organic acids and inorganic salts on cloud droplet activation. Atmos. Chem. Phys. 11, 3895–3911 (2011).

31. 31.

Sorjamaa, R. et al. The role of surfactants in Köhler theory reconsidered. Atmos. Chem. Phys. 4, 2107–2117 (2004).

32. 32.

Padró, L. T. et al. Investigation of cloud condensation nuclei properties and droplet growth kinetics of the water-soluble aerosol fraction in Mexico City. J. Geophys. Res. 115, D09204 (2010).

33. 33.

Wex, H., Stratmann, F., Topping, D. & McFiggans, G. The Kelvin versus the Raoult Term in the Köhler Equation. J. Atmos. Sci. 65, 4004–4016 (2008).

34. 34.

Dusek, U. et al. Water uptake by biomass burning aerosol at sub- and supersaturated conditions: closure studies and implications for the role of organics. Atmos. Chem. Phys. 11, 9519–9532 (2011).

35. 35.

Li, Z., Williams, A. L. & Rood, M. J. Influence of Soluble Surfactant Properties on the Activation of Aerosol Particles Containing Inorganic Solute. J. Atmos. Sci. 55, 1859–1866 (1998).

36. 36.

Gunthe, S. S. et al. Cloud condensation nuclei (CCN) from fresh and aged air pollution in the megacity region of Beijing. Atmos. Chem. Phys. 11, 11023–11039 (2011).

37. 37.

Sullivan, R. C. et al. Effect of chemical mixing state on the hygroscopicity and cloud nucleation properties of calcium mineral dust particles. Atmos. Chem. Phys. 9, 3303–3316 (2009).

38. 38.

Renbaum-Wolff, L. et al. Observations and implications of liquid–liquid phase separation at high relative humidities in secondary organic material produced by α-pinene ozonolysis without inorganic salts. Atmos. Chem. Phys. 16, 7969–7979 (2016).

39. 39.

Ma, S. X. et al. α-Pinene nitrates: synthesis, yields and atmospheric chemistry. Atmos. Chem. Phys. 11, 6337–6347 (2011).

40. 40.

Suda, S. R. et al. Influence of Functional Groups on Organic Aerosol Cloud Condensation Nucleus Activity. Environ. Sci. Technol. 48, 10182–10190 (2014).

41. 41.

Petters, M. D., Kreidenweis, S. M. & Ziemann, P. J. Prediction of cloud condensation nuclei activity for organic compounds using functional group contribution methods. Geosci. Model Dev. 9, 111–124 (2016).

42. 42.

Hiura, T. Estimation of aboveground biomass and net biomass increment in a cool temperate forest on a landscape scale. Ecol. Res. 20, 271–277 (2005).

43. 43.

Shibata, H., Kirikae, M., Tanaka, Y., Sakuma, T. & Hatano, R. Proton Budgets of Forest Ecosystems on Volcanogenous Regosols in Hokkaido, Northern Japan. Water. Air. Soil Pollut. 105, 63–72 (1998).

44. 44.

Miyazaki, Y. et al. Evidence of formation of submicrometer water-soluble organic aerosols at a deciduous forest site in northern Japan in summer. J. Geophys. Res. Atmos. 117, D19213, doi:10.1029/2012JD018250 (2012).

45. 45.

Roberts, G. C. & Nenes, A. A Continuous-Flow Streamwise Thermal-Gradient CCN Chamber for Atmospheric Measurements. Aerosol Sci. Technol. 39, 206–221 (2005).

46. 46.

Moore, R. H., Nenes, A. & Medina, J. Scanning Mobility CCN Analysis—A Method for Fast Measurements of Size-Resolved CCN Distributions and Activation Kinetics. Aerosol Sci. Technol. 44, 861–871 (2010).

47. 47.

Rose, D. et al. Calibration and measurement uncertainties of a continuous-flow cloud condensation nuclei counter (DMT-CCNC): CCN activation of ammonium sulfate and sodium chloride aerosol particles in theory and experiment. Atmos. Chem. Phys. 8, 1153–1179 (2008).

48. 48.

Miyazaki, Y. et al. Seasonal cycles of water-soluble organic nitrogen aerosols in a deciduous broadleaf forest in northern Japan. J. Geophys. Res. Atmos. 119, 1440–1454 (2014).

49. 49.

Yttri, K. E. et al. Elemental and organic carbon in PM10: a one year measurement campaign within the European Monitoring and Evaluation Programme EMEP. Atmos. Chem. Phys. 7, 5711–5725 (2007).

50. 50.

Finessi, E. et al. Determination of the biogenic secondary organic aerosol fraction in the boreal forest by NMR spectroscopy. Atmos. Chem. Phys. 12, 941–959 (2012).

51. 51.

Miyazaki, Y., Aggarwal, S. G., Singh, K., Gupta, P. K. & Kawamura, K. Dicarboxylic acids and water-soluble organic carbon in aerosols in New Delhi, India, in winter: Characteristics and formation processes. J. Geophys. Res. 114, D19206, doi:10.1029/2009JD011790 (2009).

52. 52.

Norris, G., Duvall, R., Brown, S. & Bai, S. EPA Positive Matrix Factorization (PMF) 5.0 Fundamentals and User Guide (2014).

53. 53.

Reff, A., Eberly, S. I. & Bhave, P. V. Receptor modeling of ambient particulate matter data using positive matrix factorization: review of existing methods. J. Air Waste Manag. Assoc. 57, 146–154 (2007).

54. 54.

Paatero, P. & Hopke, P. K. Discarding or downweighting high-noise variables in factor analytic models. Anal. Chim. Acta 490, 277–289 (2003).

55. 55.

Paatero, P., Eberly, S., Brown, S. G. & Norris, G. A. Methods for estimating uncertainty in factor analytic solutions. Atmos. Meas. Tech. 7, 781–797 (2014).

56. 56.

Dusek, U. et al. Enhanced organic mass fraction and decreased hygroscopicity of cloud condensation nuclei (CCN) during new particle formation events. Geophys. Res. Lett. 37, L03804, doi:10.1029/2009GL040930 (2010).

Download references

## Acknowledgements

This research was supported by Grants-in-Aid for Scientific Research (B) (25281002, 25292079, and 16H0293106) and Scientific Research (S) (24221001) from the Ministry of Education, Culture, Sports, Science and Technology (MEXT), Japan. The study was also supported by the Sumitomo Foundation in Japan. We thank H. Kawakami and T. Takeuchi for their help with the chemical analysis of the samples and M. Mochida for his advice on CCN measurements. The authors thank S.K.R. Boreddy for his helpful comments on the manuscript.

## Author information

### Affiliations

1. #### Institute of Low Temperature Science, Hokkaido University, Sapporo, 060-0819, Japan

• Astrid Müller
• , Yuzo Miyazaki
• , Eri Tachibana
•  & Kimitaka Kawamura
2. #### Graduate School of Environmental Science, Hokkaido University, Sapporo, 060-0810, Japan

• Astrid Müller
3. #### Chubu Institute for Advanced Studies, Chubu University, Kasugai, 487-8501, Japan

• Kimitaka Kawamura
4. #### Field Science Center for Northern Biosphere, Hokkaido University, Tomakomai, 053-0035, Japan

• Tsutom Hiura

### Contributions

Y.M. designed the research and led the overall study. A.M. and Y.M. performed the experiments and wrote the manuscript. T.H. coordinated the aerosol sampling at the research site. K.K. managed the CCN measurements. A.M., Y.M., and E.T. analyzed the data with significant contributions from T.H.

### Competing Interests

The authors declare that they have no competing interests.

### Corresponding author

Correspondence to Yuzo Miyazaki.

## Comments

By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.

Open Access This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article’s Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/.