Associate Editor: Joël Savarino; Laboratoire de Glaciologie et Géophysique de l’Environnement, CNRS/Grenoble University, Saint-Martin d’Hères, France
The Arctic is warming more rapidly than other regions of the world (ACIA, 2005), and a significant increase in anthropogenic activities in the Arctic is expected by mid-century if not before (Smith and Stephenson, 2013) that will further contribute to the changing Arctic climate. While much has been speculated about the role of anthropogenic black carbon in Arctic warming (UNEP, 2011), the shortwave cooling effect of the Arctic summertime aerosol and the potential response of its origins to warmer temperatures and reduced ice cover have only been scarcely studied (Curry, 1995; Mauritsen et al., 2011). Proposed some time ago as the background aerosol of the Northern Hemisphere (NH) (Megaw and Flyger, 1973), the summertime Arctic aerosol is well known to be influenced by products of the atmospheric oxidation of DMS (e.g. Sharma et al., 2012).
Oceanic emissions of DMS constitute approximately 25% of the total global sulfur emissions that enter the atmosphere (Lana et al., 2011). Once in the atmosphere, DMS is oxidized primarily to methane sulfonic acid (MSA) and sulfur dioxide (SO2), and the SO2 can be further oxidized to H2SO4 that can form new particles. MSA has some possibility of contributing to new particle formation (NPF), but its ability to nucleate is much lower than that of H2SO4 due to a higher saturation vapor pressure. Generally, MSA is considered to be relatively unimportant for NPF under atmospheric conditions (e.g. Kreidenweis and Seinfeld, 1988; Wyslouzil et al., 1991; Van Dingenen and Raes, 1993; Berresheim et al., 2002). As a condensable product of DMS oxidation, MSA is a tracer for linking particles with DMS. In addition to being oxidized in the gas phase, SO2 can also be oxidized in cloud water (e.g. Seinfeld and Pandis, 1997). The addition of H2SO4 to cloud-activated particles from the aqueous-phase oxidation of SO2 will increase the size of the activated particles following cloud evaporation. That process can lead to the development of a mode in the particle size distribution following cloud evaporation (Hoppel, Fitzgerald, and Larson, 1985), for which there is also evidence in the summertime Arctic atmosphere (Heintzenberg and Leck, 1994; Heintzenberg and Leck, 2012).
It was hypothesized many years ago that newly formed particles resulting from DMS oxidation can grow by the condensation of gases, aqueous processes in cloud, and through self coagulation to sizes where they may act as CCN and influence cloud albedo (Charlson et al., 1987). Evidence that DMS contributes to NPF in the free troposphere of the NH as hypothesized by Raes (1995) has been found by Clarke et al. (1998). Additionally, CCN in the Southern Hemisphere marine boundary layer has been linked to MSA (Ayers and Gras, 1991). However, some summertime Arctic observations have been used to question the importance of DMS in defining the aerosol number concentration and ultimately the CCN number concentration (Leck and Bigg, 2007). Further a review of many years of investigation finds little evidence to support NPF from DMS oxidation in the atmospheric boundary layer of the NH and their growth to CCN sizes (Quinn and Bates, 2011); for many areas of the world and the low atmospheric concentrations of the distributed DMS, H2SO4 derived from DMS oxidation will preferentially condense on existing particles before forming new particles (Kreidenweis et al., 1991; Pirjola et al., 2000).
Atmospheric aerosol particles, such as sea salt particles or those derived from anthropogenic sources, act as sinks for condensable gases (e.g. H2SO4) and as sites for losses of newly formed particles by coagulation. NPF derived from pervasive but low-concentration precursors, such as DMS, and subsequent growth of new particles to CCN sizes is enhanced when the above sinks are small (Kreidenweis et al., 1991; Pirjola et al., 2000). The summertime Arctic is relatively free of condensation and coagulation sinks because of increased wet deposition of particles and the more northerly position of the Arctic front that separates the Arctic air mass from mid-latitudes and inhibits the replenishment of particles from major anthropogenic source regions (Barrie, 1986; Engvall et al., 2008; Garrett et al., 2011; Stohl, 2006). Arctic observations have shown that new particles will appear following cleansing of the air by precipitation (Hogan, Barnard, and Winters, 1982), and Engvall et al. (2008) identified a reduction in the condensation sink as a major component of the shift in the aerosol size distribution from larger to smaller particles as the Arctic air transitions to less influence of anthropogenic sources during April to June.
Here, one year of observations of the submicron aerosol conducted from March, 2011 to March, 2012 at the Dr. Neil Trivett Global Atmosphere Watch (GAW) Observatory at Alert, Nunavut (82.5°N, 75°W; elevation 210 m-MSL) and simulations from the GEOS-Chem-TOMAS global chemical transport model provide evidence of a link between DMS and the particles that will serve as CCN during the Arctic summer.
The ambient aerosol is pulled into the Alert GAW laboratory through a 3 m long, 10 cm diameter vertical manifold at a flow rate of about 1000 L/min. Particles are sampled out of the manifold from near the center of the flowstream, about 30 cm up from the bottom of the manifold. From there the particles are delivered to the sampling devices via stainless steel tubing. The mean total residence time of a particle from outside to its measurement point is approximately 3 s, and at the point of sampling the aerosol is at approximately room temperature and the relative humidity (RH) is <50%.
Total number concentrations of particles >4 nm are measured using a TSI 3772 Condensation Particle Counter (CPC), and particle size distributions from 20 nm to 500 nm diameter are measured with a TSI 3034 Scanning Mobility Particle System (SMPS), verified on site using monodisperse particles of polystyrene latex and of ammonium sulfate generated with a Brechtel Manufacturing Incorporated (BMI) Scanning Electrical Mobility Spectrometer (SEMS). Particle number concentrations approximately in the size range of 4 nm to 20 nm (N4–20) are derived from the difference of the CPC and the SMPS totals.
Ten minute averaged refractory black carbon (rBC) number concentrations are measured with a Droplet Measurement Technologies Single Particle Soot Photometer (SP2) that simultaneously measures the scattering and incandescence of individual rBC particles from an intracavity Nd:YAG laser (λ=1064 nm) (Stephens, Turner, and Sandberg, 2003; Schwarz et al., 2006). The measured limit of particle size detection, based on calibration with size-selected particles of Aquadag, is a volume equivalent diameter of approximately 63 nm.
Measurements of the half-hour averaged non-refractory chemical components (mostly sulphates, nitrates and total organics) of particles smaller than 700 nm vacuum aerodynamic diameter are made with an Aerodyne Research Inc. Aerosol Chemical Speciation Monitor (ACSM) (Ng et al., 2011). On-site calibrations of the ACSM are done with nearly monodisperse particles of ammonium nitrate selected using the BMI SEMS. ACSM measurements at Alert are available for March to May, 2011; data after May to the end of the sampling period discussed here are unavailable due to instrument problems.
The real-time measurements were averaged to produce one hour data points. Those hourly averages were further discriminated for ambient RH <90% to eliminate the direct influence of water fogs; ice crystals present at RH <90% could still inhibit NPF, more so in the spring than the summer. Data with winds from 0° to 45° true north are excluded due to the potential for contamination from the Alert station approximately 10 km from the site. As discussed in the results and discussion section, the anthropogenic influence is further minimized by discrimination based on the rBC number concentrations.
Samples of total suspended particles for analysis of major inorganic ions and MSA by ion chromatography (IC) are collected on weekly integrated high volume Whatman 41 filters sampled near the ground about 50 m from the GAW lab (Sharma et al., 2012). In addition, weekly Teflon and quartz fibre filters located inside the GAW lab sample the ambient aerosol via the above inlet with a 1 µm upper size limit. Details of the high volume sample handling, analytical methods and quality control are discussed elsewhere (Li and Barrie, 1993). The Teflon filters are analyzed by IC for inorganics and MSA, using the same method as for the high volume filters, and the quartz filters are analyzed for organic carbon and elemental carbon (OC/EC) by thermal volatilization (Huang et al., 2006; Chan et al., 2010). Sulfur isotopic analyses were conducted on portions of the high volume filters collected from 1993 to 2003 as described by Norman et al. (1999).
Predictions of N4–20 particles and particle size distributions are made with version 8.02.02 of the GEOS-Chem chemical transport model (http://www.geos-chem.org). The model was configured for 30 vertical layers and run globally with a horizontal grid resolution of 4°×5°. GEOS-Chem is extended to simulate particle microphysics by adding the TwO-Moment Aerosol Sectional (TOMAS) microphysics model (Adams and Seinfeld, 2002; Trivitayanurak et al., 2008; Snow-Kropla et al., 2011); recent updates of TOMAS are documented by Pierce and Adams (2009). We use GEOS3 meteorology for the year 2001, and DMS emissions are calculated using monthly mean seawater DMS concentrations from Kettle et al. (1999) and the transfer velocity calculated using Liss and Merlivat (1986). The Kettle et al. (1999) emissions scheme used in GEOSCHEM results in global simulations of DMS emissions and atmospheric burdens that are the lowest compared with two other approaches used in GEOSCHEM and fall near mid-range of published global DMS emissions (Hezel et al., 2011); the use of the Liss and Merlivat (1986) scheme is another factor contributing to reduced DMS emissions. The Hezel et al. (2011) study also shows GEOSCHEM-simulated global atmospheric burdens of MSA are at the higher end of the published range, the austral summer MSA is about three times higher than observed MSA, the global burden of non-sea-salt sulfate is at the lower end of the published range, the austral summer non-sea-salt sulfate is approximately 50% higher than observed, and the austral summer DMS concentrations are overestimated by a factor of two. Overestimation of DMS, MSA and sulfate (derived from DMS) may also apply to the Arctic region (Kettle and Andreas, 2000). Other emissions are described by van Donkelaar et al. (2008), who also present comparisons with airborne observations that demonstrate the ability of GEOSCHEM to reasonably represent aerosol chemical mass transport across the North Pacific Ocean. This version of TOMAS, which extends the aerosol particle mass transport to number and size, has 40 size bins representing dry aerosol diameters from 1 nm to 10 µm. Aerosol chemical species incorporated into TOMAS include sulfate, sea-salt, organic carbon, black carbon and dust. The sulfur chemistry in GEOS-Chem is based on that of the GOCART model with reactions described in Chin et al. (2000). For gas-phase sulfur oxidation, DMS is oxidized by OH to form SO2 and MSA, DMS is oxidized by nitrate radicals (NO3) to form SO2, and SO2 is oxidized by OH to form sulfate. Rate constants are from DeMore et al. (1997) with yields of SO2 and MSA for DMS oxidation from Chatfield and Crutzen (1990). For aqueous-phase sulfur oxidation, SO2 is oxidized by O3 and H2O2 in clouds to form sulfate. The rate constants are from Jacob (1986). Secondary Organic Aerosol (SOA) is formed from terrestrial biogenic sources only (10% of monoterpene emissions in GEOS-Chem are converted instantly to SOA giving an annual flux of 18 Tg yr-1); one evaluation of biogenic SOA simulated by GEOS-CHEM is given by Wainwright et al. (2012). SOA is assumed to be non-volatile and is distributed across the aerosol size distribution proportionally to the Fuchs-corrected aerosol surface area (Pierce et al., 2011; Riipinen et al., 2011). Nucleation rates are predicted using the activation nucleation formulation of Sihto et al. (2006): (1) where J is the nucleation rate of 1 nm particles and A [s-1] is an empirical constant. Values of “A” of 1x10-7 (Chang et al., 2011a) and 2 × 10-6 s-1 are used here based (Sihto et al., 2006; Riipinen et al., 2007; Spracklen et al., 2008). The simulation was spun up for 1 month followed by a 12-month simulation. The aerosol size distribution and size-resolved aerosol composition was output for Alert every 6 hours for the surface model layer. Recently, aerosol size distributions predicted from GEOSCHEM-TOMAS have been compared with observations from several locations in the northern hemisphere, including Alert, indicating that the model can reasonably simulate the aerosol particle microphysics (D’Andrea et al., 2013).
An adiabatic aerosol-cloud parcel model (Shantz et al., 2010) is used to estimate CDNC from the observed aerosol number size distributions. The model has been shown to re-produce observed CDNC in near adiabatic situations and for low stratiform cloud (Leaitch et al., 2010) as found in the Arctic summer. The model incorporates the kappa parameterization (κ) to represent the particle hygroscopicity (Petters and Kreidenweis, 2007); κ can be calculated for some chemical components, but for many it is empirically determined. The values of kappa used here (0.2 and 0.5) represent a more organic dominated particle (κ=0.2) and a more sulfate dominated particle (κ=0.5) as observed in the summer Arctic (Chang et al., 2011b) as well as at Alert during May of 2011 with the ACSM (Supplemental Material S1). The parcel lifting to form the simulated cloud is based on an updraft speed of 0.4 m s-1 as observed in clouds over north Alaska in April (Earle et al., 2011).
Results and discussion
The annual pattern of the aerosol chemistry at Alert is shown in Figure 1a as the monthly averaged mass concentrations of sulfate, organic carbon (OC), elemental carbon (EC), sodium and MSA. The well-known Arctic Haze, aerosol transported from distant anthropogenic sources (e.g. Barrie, 1986), is evident in the higher concentrations of sulfate, OC and EC during the winter and early spring. April to May is a transition period when sulfate decreases and MSA from northern ocean sources becomes relatively important at Alert (e.g. Sharma et al., 2012). During July and August, the mean MSA to sulfate ratio is approximately 12% compared with a 10-year MSA to DMS-derived sulfate ratio of 39% (±21%) also for the months of July and August (Norman et al., 1999), indicating some fraction of the sulfate remains of anthropogenic origin. During July, August and September, the 10-year mean isotope-based ratio of biogenic sulfate to total sulfate is 30–40% (Figure 1b). Sodium, an indicator of sea salt, has a monthly variation similar to sulfate and decreases significantly during June, July, August and September (JJAS). Low levels of calcium in particles with diameters greater than 1 µm measured during JJAS range from 0.04–0.28 µg m-3 and are attributed to local wind blown dust impacting the ground-level field sampler.
The monthly mean particle number concentrations are shown in Figure 1b. During JJAS, the increase in the number concentrations of N4–20 particles, a potential indicator of NPF, coincides with the decline in the number concentrations of rBC particles (monthly averaged rBC and filter EC correlate with R2=0.80 and p<0.0002) and in the total particles between 200 nm and 500 nm diameter (N200; the N200 and the volume concentration of particles <500 nm correlate with R2>0.99, p<0.0001). The monthly co-variance of rBC, N200 and sulfate, all of which decrease from the spring through the summer, implies a decreasing influence from anthropogenic sources. Although MSA increases in April, the N4–20 particles do not increase until June, when the indicators of condensation sinks (sodium, N200 and possibly ice crystals) are reduced.
The impact of reduced condensation sinks on the N4–20 particles is evident in a plot of their number concentrations versus the total volume concentrations of particles <500 nm (Figure 2a). For JJAS, the N4–20 increase for volume concentrations approaching near zero. Below a volume concentration of 0.2 µm3 cm-3 the increase in N4–20 is largely associated with rBC number concentrations less than the median JJAS rBC concentration of 0.71 cm-3. The numbers of hourly averaged observations of rBC number concentrations <2 cm-3, shown in Figure 2b, indicate that the cleanest conditions are prevalent only during JJAS as represented by an increase in the number of rBC observations below the median JJAS rBC number concentration. The increase in the number of rBC observations below the JJAS median concentration represents aerosols that have undergone considerable scavenging and had no recent input from combustion sources. It is concluded that most of the N4–20 particles during JJAS were not directly related to combustion. The few scattered pink points at higher volume concentrations in Figure 2a are possibly due to local emissions that escaped filtering by wind sector; their associated rBC concentrations range from 8–32 cm-3. The results for all other months give few indications of increases in N4–20, in part due to the absence of actinic radiation, as Alert experiences 24-hour darkness from October to March.
The associations of the N4–20 with increased MSA and minimal anthropogenic influence, also observed at the Arctic site of Spitzbergen (Heintzenberg and Leck, 1994), implies that those particles are the result of NPF arising from the oxidation of DMS-derived SO2. Further, that pattern of increased NPF with decreasing existing particle concentrations has been predicted for particle formation from DMS (Kreidenweis et al., 1991). Spring and summer sources of DMS and DMS oxidation products to Alert arrive from open ocean regions, possibly enhanced near ice edges of the Arctic Ocean (e.g. see discussions by Sharma et al., 2012 and Leck and Persson, 1996). Increased levels of DMS has also been observed at higher altitudes (Lundén et al., 2010), and katabatic flows or milder forms of subsidence may be another source of DMS or its products to Alert. Two-day back trajectory analyses from the online NOAA Hysplit model (Draxler and Hess, 1997; Draxler and Hess, 1998; Draxler, 1999; Draxler and Rolph, 2013; Rolph, 2013) for JJAS show a predominance of air arriving to Alert from north across the ocean ice pack, from the south over the Canadian Arctic Archipelago and up the Nares Strait between Ellesmere Island and Greenland (Supplemental Material Figure S2). In particular, a number of trajectories descend off Greenland, from which some of the cleanest aerosol at Alert arrives and where MSA concentrations during the summer range up to 0.025 µg m-3 (Jaffrezo et al., 1994), comparable to values measured at Alert.
It has been suggested that many of the particles (and CCN) smaller than 100 nm in the summertime Arctic originate from primary emissions of biological particles (microgels) from the ocean as opposed to NPF (Leck and Bigg, 1999; Leck and Bigg, 2005; Leck and Bigg, 2010; Orellana et al., 2011). The possibility that such a process may be important in some regions of the Arctic is not disputed. However, the primary emissions of microgels does not explain the Alert observations of an increase in the N4–20 nm particles with decreasing particle volume (Figure 2a): such particles would need to be transported long distances with little modification (by growth, coagulation or deposition) and only during the cleanest periods to support the observations of Figure 2a, a possibility that is less likely than the NPF hypothesis. Consistent with prior Arctic observations (Heintzenberg and Leck, 1994), the N4–20 at Alert during JJAS were observed in excess of 106 cm-3 and 301 cm-3 50% and 25% of the time respectively, when the rBC concentrations were below their median value for JJAS of 0.71 cm-3. That frequency of N4–20 particles at Alert argues for the more likely occurrence of NPF in the atmosphere near the observation site where their likelihood of survival to detection is higher, particularly since the viability of NPF associated with DMS and a reduced condensation sink has been both predicted and demonstrated for the Arctic summertime (e.g. Hogan et al., 1982; Kreidenweis et al., 1991; Engvall et al., 2008; Chang et al., 2011a; Rempillo et al., 2011) as well as elsewhere in ultra-clean environments (Petters et al., 2005; Wood et al., 2011). Thus, these results offer evidence for the common occurrence of NPF in the Arctic summertime boundary layer linked with DMS, previously considered to be an unlikely possibility for the NH (Pirjola et al., 2000).
Simulations of NPF at Alert were conducted with GEOS-Chem-TOMAS for two values of the ‘A’ factor (equation 1). Using the value of 1 × 10-7 for ‘A’ (Chang et al., 2011a) yielded no significant NPF (not shown). With the value of 2 × 10-6 for ‘A’ (Sihto et al., 2006), the modeled pattern of the N4–20 particles versus volume for Alert (Figure 3a) is similar to that observed at Alert with the exception that the model does not clean the atmosphere around Alert as much as indicated by the observations. The model simulates few volume concentrations below 0.1 µm3 cm-3 and most of the simulated NPF occurs between volume concentrations of 0.1 µm3 cm-3 and 0.3 µm3 cm-3, whereas the observations indicate nucleation occurs predominantly at volume concentrations below 0.1 µm3 cm-3. The resulting higher simulated condensation sink will require a larger value of ‘A’ than might be interpreted from a box model initiated with local observations (e.g. Karl et al., 2012). As discussed by Sihto et al. (2006) and Chang et al. (2011a), ‘A’ is potentially influenced by a large number of factors, (e.g. condensation sink, VOCs, NH3, OH and SO2 branching from DMS oxidation), which makes its determination highly variable. For example, the Sihto et al. (2006) value is the mean of several ambient measurements at Hyytiälä (near 62°N) during mid-March to early April that vary from 4 × 10-7 to 6 × 10-6, and Riipinen et al. (2007) found a mean value of 2.4 × 10-7 (range 3.3 × 10-8 to 2 × 10-6) for ‘A’ at the same site for April to May. Further, chamber observations suggest that atmospheric nucleation rates may strongly depend on the availability of small concentrations of gas-phase amines (Almeida et al., 2013). It is concluded that the simulated results shown in Figure 3a support the concept that the reduced condensation sink under the clean summertime conditions at Alert promotes NPF. Further, the results shown in Figure 3b indicate viability of NPF from the oxidation of SO2 that is derived from the oxidation of DMS.
NPF is important for climate only if some of the newly formed particles grow to sizes where they can significantly affect either atmospheric light extinction or the number concentrations of cloud droplets (Forster et al., 2007). As shown below, particles from 50–60 nm and larger may nucleate cloud droplets in the clean summertime Arctic. At Alert, the number concentrations of particles larger than 60 nm (N60) and larger than 100 nm (N100) increased from June through September relative to N200, and for the cases with rBC <0.71 cm-3 the absolute values of N60 and N100 increased from June through August by 3–4 times (Figure 4a). Kinetically, the growth of newly formed particles to 60 nm diameter for the conditions of the Arctic summertime may occur within about one day (Chang et al., 2011a). Also, a DMS source can explain the mass of the smaller particles at Alert. For rBC <0.71 cm-3, the July and August means of the integrated volume concentrations are 0.014 µm3 cm-3 and 0.047 µm3 cm-3 for particles in the size ranges of 20–100 nm and 20–200 nm respectively. Those values convert to sulfate mass concentrations of approximately 0.025 µg m-3 and 0.084 µg m-3, respectively, estimates that are consistent with the Arctic observations of Chang et al. (2011b). Considering the observed mean MSA concentration of about 0.01 µg m-3 (Figure 1) and the ratio of MSA to DMS-derived sulfate (0.39) (Norman et al., 1999), the estimated mean mass of MSA plus DMS-derived sulfate is about 0.026 µg m-3 or 31% of the above value for 20–200 nm particles. Thus, it is possible that a significant fraction of the material that grew the 20–200 nm particles originated from DMS. DMS-related growth of the particles is also supported by the GEOS-Chem-TOMAS simulations that indicate an increase in N100 associated with DMS of between 15 cm-3 and 25 cm-3 during JJAS (Figure 4b). Those number concentrations compare with the N100 particles for the JJAS cleaner periods of 5 cm-3 to 30 cm-3 (Figure 4a). The growth of newly formed particles to CCN sizes is not necessarily restricted to sulfur components. The submicron concentrations of organic carbon mass (OC; Figure 1a) and total organic mass (OM; Supplemental Material Figure S1) here and elsewhere in the summer Arctic (Chang et al., 2011b) are comparable to those of sulfate during the summer indicating that other marine sources, including emissions of volatile organic compounds, likely contributed to the evolution of the particles (Karl et al., 2012; Russell et al., 2010; Shaw, Gantt, and Meskhidze, 2010; Fu et al., 2009; Leck et al., 2002; Heintzenberg and Leck, 2012).
The MSA mass concentrations simulated by GEOSCHEM for Alert (Figure 3) are an order of magnitude higher than the observed concentrations (Figure 1). As discussed in Modeling Methods, DMS, MSA and sulfate (from DMS) may be over estimated in the POLAR regions (Kettle and Andreas, 2000; Hezel et al., 2011), suggesting that DMS-derived sulfate mass concentrations are also over predicted. Potentially higher model concentrations of DMS-derived SO2 may contribute to the higher modeled N4–20; the monthly mean modeled N4–20 for June and July are 1912 cm-3 and 878 cm-3, respectively, whereas the monthly means of the observed N4–20 are 339 cm-3 and 200 cm-3 for June and July respectively. The GEOSCHEM simulations under predict the organic mass in the Alert submicron aerosol relative to the observations (not shown), which may explain the relatively close agreement of the simulated and observed N100 concentrations despite an apparent over prediction of sulfur from DMS. Despite these limitations, the GEOSCHEM simulations support the conclusion that the growth of particles in the relatively clean air is consistent with marine sources.
The monthly mean JJAS particle number distributions for lower rBC (<0.71 cm-3) and higher rBC (>0.71 cm-3) are shown in Figure 5. With the gradual cleansing of the anthropogenic aerosol over the summer period, the number of hours with lower rBC become an increasingly larger fraction of the total monthly hours. The lower September aerosol concentrations in both cases are a product of 1) increased wet deposition during August and September when cloud and precipitation were prevalent compared with July for which no precipitation was recorded, 2) reduced DMS fluxes in the Arctic (Lana et al., 2011) and 3) the minimal anthropogenic influence as represented by the lowest mean rBC concentrations (Figure 1). The 80–200 nm mode in the August lower-rBC distribution, seen elsewhere in the Arctic summer, suggests the addition of sulfate to the cloud activated particles via aqueous-phase oxidation of SO2 (Heintzenberg and Leck, 1994; Heintzenberg and Leck, 2012; Hoppel, Fitzgerald, and Larson, 1985). The lower-rBC distributions of JJA were input to the aerosol-cloud parcel model to estimate credible CDNC. The ranges of the minimum predicted sizes at which particles activate to cloud droplets are shaded in Figure 5a. The predicted CDNC of 24–30 cm-3, 45–63 cm-3 and 53–68 cm-3, for June, July and August respectively, fall in the lower end of the range of modelled global mean pre-industrial CDNC (30–140 cm-3) (Penner et al., 2006). Thus both predictions of CDNC from a natural source, one of which is founded on observational data, are consistent. The predicted CDNC are higher in August than in June by 23–44 cm-3, comparable to the <50 cm-3 increase in the global mean CDNC needed to give rise to a similar cloud albedo as the cloud albedo forcing from industrial aerosols (Penner et al., 2006). These results suggest that DMS may be a defining factor in much of the summertime Arctic low cloud microphysics and potentially has a significant influence on the shortwave albedo of low clouds during the Arctic summer.
Cleansing of the summertime Arctic atmosphere can trigger new particle formation. Modest growth of the new particles via gas- and aqueous-phase processing increases the number concentrations of those particles that will serve as nuclei for cloud droplets (CCN). An associated increase of methane sulfonic acid (MSA) and a decrease of refractory black carbon particles combined with simulations from the GEOS-Chem-TOMAS global model lead to the conclusion that dimethyl sulfide (DMS) may play a defining role in the size distribution of the clean summertime Arctic aerosol at Alert. For half of the days during July and August of 2011, DMS sources are estimated to have been the main origin of CCN at Alert, and provide one baseline estimate for the aerosol cloud albedo effect. Since the 2011 MSA concentrations were close to the 30-year mean (0.09 µg m-3) (Sharma et al., 2012), it is possible that DMS may in general have a significant impact on summertime Arctic clouds. The relative increase in the contribution from DMS to CCN from June through August is connected to a diminishing anthropogenic contribution over the same period. New sources of particles and CCN from expected increases in anthropogenic activities in the Arctic in coming years are likely to lessen the natural influence and weaken our ability to make such estimates.
Data accessibility statement
The primary data are included in spreadsheets as part of the supplemental material.
Supplemental material legendsFigure S1.
Time series of the particle chemistry from the ACSM compared with the SMPS volume concentration.
File Type: DOC
File Size: 0.106 MB
Daily back trajectories air parcels arriving at Alert during June, July, August and September, 2011 from the NOAA Hysplit model. (XLS)
File Type: XLS
File Size: 13.954 MB
© 2013 Leaitch et al. This is an open-access article distributed under the terms of the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original author and source are credited.
Contributed to conception and design: WRL, JRP
Contributed to acquisition of data: WRL, SS, LH, DT-S, AC, JRP, NCS, A-LN
Contributed to analysis and interpretation of data: WRL, AMM, KvS, JRP, AKB, JS, NCS, RY-WC, A-LN
Drafted and/or revised the article: WRL
Approved the submitted version for publication: All
There are no competing interests.