Submicron aerosol size distributions, CN and CCN concentrations at a constant supersaturation of 0.6% were measured at a relatively remote coastal site at Gosan in Jeju Island, Korea, during the ABC-EAREX from 11 March to 8 April 2005. The average CN concentrations were 6088 ± 3988, 5231 ± 2454 and 3513 ± 1790 cm−3, respectively, for the three major air mass types classified by their origins. The corresponding CCN concentrations were 2393 ± 1156, 2897 ± 1226 and 1843 ± 585 cm−3. The type III air mass was the closest to maritime origins, but these lowest concentrations at Gosan were an order of magnitude higher than those of clean marine boundary layer, indicating that regardless of air mass designation springtime submicron aerosols at Gosan were under steady continental influences. Distinct new particle formation and growth events occurred on 6 d, when clear sky weather conditions prevailed that brought air from northern China, Mongolia or Russia by anticyclonic circulations. Simultaneous occurrence of these events at a western coastal site in the Korean Peninsula 350 km north of Gosan suggests that these events were not local but at least regional-scale events. CCN concentrations were predicted with the aerosol size distributions and the assumption of particles being composed of (NH4)2SO4. The predicted to measured CCN concentration ratio was 1.27 ± 0.29 and the r2 was 0.77 for the whole measurement period. The type I air mass that has the most continental influences showed a slight tendency to overpredict CCN concentrations but the good agreement overall suggests that springtime Gosan aerosols act almost like ammonium sulfate as far as CCN activity is concerned, almost regardless of air mass origin.
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 Submicron aerosols dominate the number concentration of atmospheric particles [Hobbs, 2000]. They encompass newly formed nanometer size particles by gas to particle conversion to large particles formed by coagulation of these small particles and gas condensation onto existing particles and also by cloud processing [e.g., Hoppel et al., 1986]. Importantly a great majority of number concentrations of atmospheric particles of anthropogenic origin belong to this size category [Seinfeld and Pandis, 1998]. The concentrations and size distributions of submicron aerosols vary greatly with geographical locations and in one location they can also temporally vary with the local source activities and transport pathways determined by meteorology [Jaenicke, 1993]. So there is intrinsic variability of submicron aerosol distributions at any given location.
 Nevertheless atmospheric submicron aerosols have been of great interest. Since their sizes are comparable to solar wavelengths, visibility is directly affected. More importantly in a climatic sense, atmospheric particles of these sizes crucially affect the solar radiation budget directly by absorption and scattering [Harshvardhan, 1993]. Moreover cloud condensation nuclei (CCN) that can be activated to become cloud droplets at water supersaturations (S) of atmospheric clouds (<1%) are mostly of these sizes; for example (NH4)2SO4 particles of 0.1% critical supersaturation (Sc) are 0.135 μm in diameter (Dp) [Pruppacher and Klett, 1997]. Since CCN concentration and composition are among the most important factors that determine cloud microphysical properties, which in turn determine cloud albedo and influence cloud lifetime and extent, solar radiation budget is indirectly affected by aerosols acting as CCN [Twomey, 1977; Albrecht, 1989].
 There have been a number of field studies in the last two decades that aimed at improving our understanding of atmospheric aerosols and their role in climate prediction [e.g., Ramanathan et al., 2001]. However, correct assessment of aerosol radiative forcing is still a formidable task because of the great spatial and temporal variability of atmospheric aerosol distributions and their optical and chemical properties. The aerosol indirect effects, which require proper understanding not only of what portion of aerosols can act as CCN but also of the atmospheric dynamics that determine cloud development, are considered to be the greatest source of uncertainties in climate prediction [Intergovernmental Panel on Climate Change, 2001].
 This study presents submicron aerosol size distributions, total particle (i.e., condensation nuclei, CN) concentrations (NCN), and CCN concentrations (NCCN) measured at a coastal site at Gosan in Jeju Island of Korea (Figure 1) during the Atmospheric Brown Clouds–East Asian Regional Experiment in 2005 (ABC-EAREX 2005), the purpose and scope of which are described in detail by T. Nakajima et al. (Overview of the ABC EAREX 2005 regional experiment and a study of the aerosol direct radiative forcing in east Asia, submitted to Journal of Geophysical Research, 2007). Fast economic growth and industrialization in China and other regions in East Asia necessarily designate the Gosan site as one of the key locations to monitor the influence of Asian continental outflow. This site was also used as a key ground measurement station during the Aerosol Characterization Experiment in Asia (ACE-Asia) conducted in April–May 2001 [Huebert et al., 2003]. The main purpose of this study is to characterize springtime submicron aerosol size distributions and CN and CCN concentrations at this coastal site, on which only a few numbers of papers have been published in scientific journals [e.g., Yum et al., 2005; Adhikari et al., 2005]. An attempt is also made to link aerosol size distributions to CCN concentrations as an effort to predict CCN concentrations from aerosol size distributions [Roberts et al., 2006]. Lacking in this study is the chemical characterization of submicron aerosols, which can be found elsewhere in this special issue.
 Measurements were made in an instrument shelter at the Gosan site located on a cliff (∼50 m ASL) at the western tip of the Jeju Island's coastline (Figure 1), which is reported to have the lowest local anthropogenic emission in Korea [Kim et al., 1998]. The instrument shelter is located about 10 m inland from the cliff edge. The site and its surrounding areas are covered with grass. The agricultural activity at the village located 1 km to the east of the site is minor. Sample air was drawn from the 6 m stainless steel inlet pipe of 15 cm diameter vertically aligned through the ceiling of the instrument shelter and then delivered to different instruments from the manifold structured to be at 90° angle with the inlet pipe. Therefore the sample air came from approximately 8 m above the ground and 58 m above the sea surface, avoiding immediate influence of sea spray particles. The whole measurement period was from 11 March to 8 April 2005 but CCN measurements ended on 30 March.
 A Scanning Mobility Particle Sizer (TSI SMPS-3936L10) measured aerosol number size distributions (10 nm < Dp < 300 nm) every 3 min with a resolution of 65 channels per decade. The manufacture-provided data inversion program with the diffusion loss correction routine was applied. Integration of SMPS measured aerosol number distribution provides total particle concentration for the given size range (NSMPS); to differentiate from NCN measured by a Condensation Particle Counter (TSI CPC-3010; Dp > 10 nm) with 1 min time resolution. Since TSI CPC-3010 model saturates at concentrations greater than 104 cm−3 because of coincidence pulses, a sample air dilution system was introduced for this measurement and then measured concentrations were multiplied by the dilution factor to calculate actual concentrations. A stream-wise thermal gradient CCN counter [Roberts and Nenes, 2005] built at Scripps Institute of Oceanography measured NCCN at a fixed S of 0.6% with a time resolution of 10 s.
 Aerosol size distributions, CN and CCN concentrations were continuously measured throughout the whole measurement period except occasional breaks of an hour or so for maintenance. There were no size distribution measurements on 27 March because of SMPS malfunctioning. CCN data were also continuous except some data had to be discarded since they were measured under improper conditions such as insufficient wetting of the column. On average CCN data were not available for 2.4 h in each CCN measurement day.
3.1. Air Mass Designation
Figure 2 shows all of the 6-hourly 3 d air mass back trajectories calculated by the HYSPLIT4 model [Draxler and Hess, 1998] for the entire measurement period, which have been classified into three major types. Type I air mass originated mostly from remote continental northern China, Mongolia or Russia and passed over the Yellow Sea before arriving at Gosan (Figure 2b). The weather patterns for these trajectories usually showed a solid high-pressure system centered in eastern China, generating northwesterly winds to the east by anticyclonic circulations. The weather at Gosan was mostly clear sky for these trajectories (Figure 3; more on this figure later). The origin of the type II air mass varied a lot but was close to coastal areas in China and Korea where the population density is high. Type II trajectories spent the majority of time over the Yellow Sea or the South China Sea before they arrived at Gosan (Figure 2c). Type III air mass originated over the sea and spent almost the entire time over the sea south of Jeju Island (Figure 2d). The weather patterns for type II and III usually showed a low-pressure system or a frontal system passing through Jeju Island and the weather was cloudy or rainy (Figure 3). Presumably type I may be classified as remote continental, type II anthropogenically modified maritime, and type III maritime but as it turns out, these classifications have only a trace of their typical characteristics and they may all be broadly classified as continental/polluted.
3.2. Aerosol Distributions
 The total and each air mass type averages of particle concentrations (NCN and NSMPS) and CCN concentration (NCCN) are listed in Table 1 and the time series of the daily averages are shown in Figure 3. Different shadings in Figure 3 represent the air mass types. Also shown is the weather report (“clear sky” or “cloudy or rainy”) for each day by the ABC science team. The weather may have varied in the middle of the day and therefore this report is sort of an overall assessment. The days when particle formation and growth events occurred were marked on the top axis and will be discussed in more detail in the next subsection.
Table 1. Averages of CN Concentrations (NCN), SMPS Concentrations (NSMPS) and Geometric Mean Diameters (Dg), CCN Concentrations (NCCN), and the NCCN/NCN Ratios for the Entire Data Set, Type I, Type II and Type III Air Massesa
Averages for type I excluding particle formation and growth event periods are also shown.
5599 ± 3518
5337 ± 3406
65 ± 19
2463 ± 1168
0.51 ± 0.18
6088 ± 3988
5805 ± 3857
60 ± 18
2393 ± 1156
0.45 ± 0.17
Type I (no event)
5008 ± 2104
4771 ± 2073
63 ± 16
2295 ± 1140
0.49 ± 0.16
5231 ± 2454
4812 ± 2240
74 ± 16
2897 ± 1226
0.60 ± 0.17
3513 ± 1790
3430 ± 1750
75 ± 18
1843 ± 585
0.62 ± 0.13
 The average NCN and NSMPS for the entire measurement period are 5599 ± 3518 cm−3 and 5337 ± 3427 cm−3, respectively (Table 1). The less than 5% difference between CPC-3010 and SMPS-3936L10 concentrations is expected, considering the fact that aerosol concentrations are usually dominated by the Aitken mode particles (say, mostly below the SMPS upper size cut of 300 nm). The average NCCN is 2463 ± 1168 cm−3. This is only 43% of NCN but the average NCCN/NCN ratio is 0.51 (Table 1, last column), which was calculated from those ratios of the corresponding 15 min average CCN and CN concentrations. This difference is due to the unavailability of CCN data after 30 March, when aerosol concentrations increased to somewhat higher values than before this date (Figure 3).
 When the three air mass types are compared in Table 1, type I has the highest average aerosol concentrations. However, if the time ranges are excluded when the aerosol concentrations were increased because of particle formation and growth events that occurred only during the type I air mass period (Figure 3), type II has slightly higher concentrations than type I. On the other hand, NCCN is significantly higher in type II than type I regardless of the exclusion of particle formation and growth event periods. This indicates that CCN are more abundant in the air masses that originated from densely populated coastal areas and having longer residence time over the sea (type II) than those from remote continental China, Mongolia or Russia (type I). One may expect that this is in some part due to the small particles that formed by nucleation and indeed NCCN/NCN ratio increased slightly when particle formation and growth periods are excluded (Table 1, last column; 0.45 ± 0.17 to 0.49 ± 0.16) but this is still significantly smaller than the NCCN/NCN for type II. The lowest aerosol concentrations are expected for type III since the 3-d back trajectories resided almost entirely over the sea (Figure 2d). However, the contribution of sea salts may be insignificant for the Gosan submicron aerosols [Maria et al., 2003].
Figure 4 shows the time evolution of the SMPS measured aerosol size distributions for the whole measurement period. The six particle formation and growth event days (Figure 3) are clearly identified. There are some other days with similar but less clear behavior and they are not counted as such event days. Except for these event periods, aerosol size distributions generally do not show distinct bimodal distributions (Figure 4). This is also evident when the average SMPS size distribution for each air mass is compared (Figure 5). The type I size distribution is somewhat bimodal with two modes at 35 nm and 90 nm (Figure 5a). When the influence of small particles during the six particle formation and growth event periods is excluded, the bimodal shape is still maintained but particle concentrations are reduced relatively more at smaller Dp ranges and the smaller mode Dp increases from 35 to 45 nm (Figure 5b). The type II size distribution shows a dominant mode at 100 nm (Figure 5c). The type III size distribution has one distinct mode at close to 80 nm (Figure 5d). The average geometric mean diameter (Dg) for each of the aerosol types is shown in Table 1. The smaller mode Dp of type III than type II but almost the same Dg of the two air masses indicate relatively larger proportion of larger particles for the type III size distribution because of the longer aging time for type III (Figure 2).
Figure 6 shows the average diurnal variations of NCN, NSMPS, and NCCN for the entire measurement period (Figure 6a) and when particle formation and growth event periods were excluded (Figure 6b). Early afternoon peak is conspicuous for NCN and NSMPS in Figure 6a because of the increase of aerosol concentrations during the particle formation and growth events that occurred on 6 d (Figure 3), which generally started near noontime and lasted for several hours to more than 10 h. The large error bars for NCN in the early afternoon hours reflect the huge daily variation of concentrations associated with new particle formation. When these event periods are excluded, diurnal variations of NCN and NSMPS are insignificant (Figure 6b). The NCCN shows negligible diurnal variation whether or not the particle formation and growth events are included (Figure 6), implying that newly formed small particles could not act as CCN because of their size limitation (more on this later). An individual particle formation and growth event day (Figure 7a) and a nonevent day (Figure 7b) are compared in Figure 7. Figure 7a shows how the particle concentrations increase and Dg suddenly falls off because of the formation of large numbers of small particles on a particle formation and growth event day, but no significant diurnal variation is obvious on a nonevent day (Figure 7b). Again NCCN shows no significant diurnal variations on the particle formation day as well as on the nonevent day.
3.3. Particle Formation and Growth Events
Figure 8 is a closer look at the diurnal variation of the SMPS measured aerosol size distributions on 14 March when a particle formation and growth event occurred. High concentrations of 10 nm particles appear at 1030 local time (LT) and the modal diameter grows as the time progresses until 0100 LT the next day. The growth curve spanning 14 h is clearly recorded. Back trajectories on this day suggest the air at Gosan surface (50 m ASL) and 500 m altitudes were coming consistently from northwest, spending the prior 24 h over the Yellow Sea. On 14 March, the measured wind at the Gosan weather station was also consistently from northwest or north with the average speed of 7 m s−1 until 8 PM when the wind direction changed to east or southeast. This is also the time when the growth curve is disrupted (Figure 8) but unlike the growth curve that returns to the original growth track after an hour, the wind direction never returned to northwest or north. This suggests that the event was not a local event but a regional event that occurred simultaneously in a large areal extent over the Yellow Sea. Assuming the wind speed of 7 m s−1, 10 h stretches translate into 250 km distance. Indeed the SMPS measurements at the Korea Global Atmosphere Watch Observatory (KGAWO) located at the west coast of the Korean Peninsula (∼350 km north of Gosan; Figure 1) did detect almost simultaneous new particle formation and growth event on this day [Lee et al., 2007]. In fact, in four out of six particle formation and growth event days at Gosan, the KGAWO also observed such events. Evidence of regional or synoptic-scale particle formation and growth events were also reported at or nearby the Gosan site during the ACE-Asia project [McNaughton et al., 2004; Buzorius et al., 2004]. Large-scale particle formation is also reported by Tunved et al.  but here the particle formation occurred during the transition from maritime to continental air mass over the northern European boreal forest and the sources of precursor gases were terpenes from the boreal forest.
 Two upper air soundings are made every day at the Gosan weather station (0900 and 2100 LT) and therefore no vertical sounding is available in the midday. The 0900 LT sounding on this day showed a neutrally stratified atmosphere up to the temperature inversion at 1900 m ASL. As the day progressed and the surface temperature increased, possibility of vertical mixing increased. Nilsson et al.  suggested that strong mixing during the rapid growth of boundary layer height caused an increase in the nucleation rates due to increases in the saturation ratios of precursor gases. From the measurement at Gosan during ACE-Asia, Buzorius et al.  showed that particles were formed in upper part of the boundary layer prior to turbulent mixing by chemically driven processes and then transported down to lower altitudes as the day progressed and the mixed layer is elevated. There is no direct evidence that the particle formation and growth event on 14 March was related to either of the two explanations. The air mass back trajectories from the Gosan surface and 500 m altitude, respectively, showed almost no variation in altitude for the previous 24 h or were below 1000 ASL for more than a day previously, indicating that particle formation occurred near the surface altitudes. Several particle formation mechanisms in various environments have been suggested [e.g., Kulmala et al., 2001, 2004; O'Dowd et al., 2002] but to find the one that fits particle formations at Gosan requires detailed chemical analysis, which is out of the scope of this study.
 Particle formation and growth events were recorded on 5 other days (Figures 3 and 4) but the events started 1 or 2 h later and thus closer to noon than the one shown in Figure 8 and lasted for 4 to 10 h. The particle growth rate (the slope of the regression line between time and mode Dp of the aerosol size distribution) for the first 4 h for the event on 14 March (Figure 8) was 3.4 nm h−1 and for the other five events it ranged from 4 to 10 nm h−1. These values are comparable to many of the measurements reported by Kulmala et al. . All six events occurred on the days that belong to type I, for which the prevailing weather conditions were clear sky (Figure 3), bringing air mostly from north or northwest directions, confirming that daytime solar radiative flux is a prerequisite for particle formation [e.g., O'Dowd et al., 2002; Lee et al., 2003]. Moreover, 1 or 2 d before the event, Jeju Island was usually under the influence of a frontal or low-pressure system, cleaning the air by cloud or precipitation scavenging and therefore reducing the preexisting surface areas that the precursor gases might condense onto [e.g., McMurry et al., 2005]. Unlike the Mace Head coastal area observations [O'Dowd et al., 2002], however, particle formation at Gosan did not coincide with the occurrence of low tide (not shown) as the rugged Gosan coastline did not expose considerable amounts of marine biota during low tides. Perhaps the sample air drawn from 58 m ASL was too far from the shore to exert significant influence on the measurement. The fact that the air was coming consistently from north or northwest where no notable landmass exists for several hundred km suggests that particle formation occurred somewhere over the Yellow Sea.
3.4. CCN: Aerosol
Figure 9 shows the scatterplots of NCN versus NCCN (Figure 9a) and NCN versus NCCN/NCN ratio for the CCN measurement period (11–30 March 2005). The average NCCN/NCN ratios are listed in Table 1. There is an increasing trend of NCCN with NCN but the NCCN/NCN ratios tend to decrease as the NCN increase, indicating that greater portions of aerosols are CCN inactive as CN concentration increases. It is hard to differentiate the three air mass types in Figure 9 but on average (Table 1) type I has the lowest NCCN/NCN and type III has slightly larger value than type II. However, NCCN varies a lot for a given NCN, especially for lower NCN (Figure 9b). This reflects the inaccuracy of estimating CCN concentrations in polluted conditions without physical and chemical information.
Roberts et al.  and several others [e.g., Bigg, 1986; Covert et al., 1998; Wood et al., 2000; Snider and Brenguier, 2000] predicted CCN concentrations at a given supersaturation based on the SMPS measured aerosol size distributions. Assuming all particles are composed solely of (NH4)2SO4, the critical dry particle diameter (Dc) can be calculated from Köhler theory [Pruppacher and Klett, 1997]. The Dc is 41 nm for Sc of 0.6%, the S setting of our CCN counter. This means that if ammonium sulfate is assumed for composition, only particles greater than 41 nm diameter can become CCN at 0.6% S. Integration of SMPS particle concentrations only for Dp greater than 41 nm provides predicted CCN concentration (NCCN,pred). Figure 10 compares measured with predicted CCN concentrations based on this premise. Figure 11 plots NCCN,pred/NCCN as a function of NCCN. Overall the correspondence is very good (Figure 10a: r2 = 0.77, y = 1.13 × +292; Figure 11a: NCCN,pred/NCCN = 1.27 ± 0.29). There is a tendency to overpredict for type I (Figure 11b; NCCN,pred/NCCN = 1.33 ± 0.30) but the correspondence for type II and III are remarkable; type II has NCCN,pred/NCCN ratio closest to one (1.10 ± 0.22) (Figure 11c) and type III has the slope of the linear regression line closest to one among all cases (1.06) (Figure 10d). Figure 7 also demonstrates that when only the particles of Dp greater than 41 nm are counted from the SMPS data, the particle concentration (N41, i.e., this is equal to NCCN,pred) follows NCCN really well on the particle formation day (Figure 7a) as well as on the nonevent day (Figure 7b). The slight overprediction for type I implies somewhat less CCN active aerosols than ammonium sulfate for this air mass. Correspondingly Maria et al.  found relatively higher fraction of organic matter (hence less soluble fraction) for the submicron aerosols of the back trajectories similar to type I than for other back trajectories. However, the good overall correspondence indicates that springtime Gosan aerosols act almost like ammonium sulfate as far as CCN activity is concerned, almost regardless of air mass origins.
 Another way to quantify CCN capability of aerosols is to compare experimentally determined critical diameter (Dc,meas) to that of ammonium sulfate (Dc,ammo) for a given S (e.g., 41 nm for 0.6% S from Köhler equation). The Dc,ammo/Dc,meas ratio is named as a CCN activation index [Roberts et al., 2006]. The integration of SMPS aerosol size distribution from the upper size limit to the Dp at which the integrated concentration equals the measured CCN concentration yields Dc,meas. The basic assumption is that particles of Dp greater than the Dc for a given S would be activated as cloud droplets and be counted as CCN by a CCN counter of the given S setting if the particle chemical composition is completely ammonium sulfate. Figure 12 plots the Dc,ammo/Dc,meas ratio as a function of NCCN. There seems to be no definite trend of Dc,ammo/Dc,meas with NCCN. A majority of the data points are in between Dc,ammo/Dc,meas of 0.5 and 1.0. For type II, however, a significant fraction of the data points are above Dc,ammo/Dc,meas of 1.0 line. This implies that some aerosols are even more CCN active than ammonium sulfate, i.e., particles of Dp smaller than the Dc of ammonium sulfate for the given S (0.6%) can serve as CCN, an excellent candidate being the sea salt particles such as sodium chloride. Overall the average Dc,ammo/Dc,meas for the entire data set is 0.79 ± 0.23 (Figure 12a).
 CN and CCN concentrations measured at other locations are summarized in Table 2. Previous measurements in northeast Asia [Song and Yum, 2004; Yum et al., 2005; Kim et al., 2005; Adhikari et al., 2005] report several thousands per cm3 of NCN. Comparable to these concentrations are the measurements at a coastal site on a remote island in eastern Mediterranean in a polluted air mass [Eleftheriadis et al., 2006] or the aircraft measurements of polluted air in the eastern Pacific [Roberts et al., 2006] and off the coast of Florida in continental air masses [Hudson and Yum, 2001]. Meanwhile O'Dowd et al.  reported significantly low typical NCN of 400–600 cm−3 at an eastern Atlantic coastal site in Mace Head although the concentration increased up to 7000 cm−3 for most polluted air. Hoppel and Frick's  central Pacific cruise measurements and Hoppel et al.'s  trans-Atlantic cruise measurements reported 300 cm−3 or less in the central part of the oceans. Similar values were found over the Southern Ocean and northeastern Atlantic [Bates et al., 2000]. Several aircraft measurements in clean marine boundary layers also reported a few hundred particles per cm3 [Hudson et al., 1998; Yum and Hudson, 2001, 2002, 2004; Hudson and Yum, 2002]. These listings suggest that the NCN measured in this study (Table 1) are comparable to or greater than coastal or marine measurements with significant continental or anthropogenic influence. The NCN of type III, supposedly least affected by anthropogenic influence, turns out to be about an order of magnitude higher than the background concentration in clean maritime environment. The lowest instantaneous CN concentration during the whole measurement period in this study was 979 cm−3 (Figure 9a), never being close to the clean maritime background concentrations listed in Table 2. However, this could very well be the background NCN in the springtime northeast Asian coastal environments.
Table 2. Summary of the Measurements in Comparison
 Measurements in the background marine boundary layer often showed distinct bimodal aerosol size distributions with the smaller mode at Dp ∼ 40 nm and the larger mode at ∼200 nm [e.g., Hoppel et al., 1990; Hoppel and Frick, 1990; Bates et al., 2000]. The larger mode peak was often enhanced by cloud processing, the mechanism of which is fully explained by Hoppel et al. [1986, 1990]. Under continental influences, the aerosol size distributions in the marine environments usually showed a unimodal shape and the mode Dp varied with the aging time over the ocean from around ∼80 nm for the least aged to ∼250 nm for aged [e.g., Hoppel et al., 1990; Bates et al., 2000; Eleftheriadis et al., 2006; Roberts et al., 2006]. Therefore the submicron aerosol size distributions measured in this study (Figures 4 and 5) is closer to continental size distributions with a little aging time rather than the distributions that were often found in clean marine boundary layer. The type I size distribution does show bimodal nature but the smaller mode is due to the contribution from newly formed small particles and not due to a solidly established Aitken mode particles that reside in the marine air without changing sizes for an extended period of time (say, more than a day [Bates et al., 2000]).
 There are reports that anthropogenically influenced air had higher NCCN/NCN than maritime air (Table 2): 0.41 versus 0.74 over the eastern Atlantic at 0.6% S [Yum and Hudson, 2002]; 0.49 versus 0.66 over the Indian Ocean at 1% S [Hudson and Yum, 2002]. Adhikari et al.  also reported NCCN/NCN ratio of 0.3 (0.3% S) or less in the relatively clean maritime air and ∼0.5 for anthropogenically influenced air. Meanwhile Yum et al.  measured 0.64 (1.0% S) that did not vary with air mass designation. Our data seems consistent with these results: on average type II and III showed almost a factor of two differences in NCN but NCCN/NCN were about the same (Table 1). However, this lack of trend was for relatively high aerosol concentrations. The lowest average NCN given by Yum et al.  and this study (type III) were even greater than the continental NCN given by Yum and Hudson  and Hudson and Yum . In fact, for NCN greater than 1000 cm−3, there seems to be a decreasing trend of NCCN/NCN with NCN for individual data points (Figure 9b). The lowest NCCN/NCN for type I in Table 1 is expected since this air mass has remote continental origin with relatively shorter marine residence time. However, the ratio itself (0.45; Table 1) seems to be still too high for remote continental air, suggesting significant anthropogenic influence even for this air mass. Hudson and Frisbie  observed NCCN/NCN ratio of 0.30 or less at 0.75% S for continental aerosols of minimal anthropogenic influence.
 The predicted CCN concentrations matched very well with the measured CCN concentrations in this study (Figure 10). This is sort of a pleasant surprise for one good reason. Our method [Roberts et al., 2006] uses only the size information and did not utilize size resolved aerosol chemistry information, which is essential to characterize CCN activity of aerosols, but still achieved CCN closure as good as or even better than some attempts did that utilized aerosol chemistry information [e.g., Chuang et al., 2000; Cantrell et al., 2000; Roberts et al., 2002; Gasparini et al., 2006]. This could only mean that the simple assumption of particles being composed solely of (NH4)2SO4 is close to the reality for the springtime northeast Asian submicron aerosols almost regardless of air mass origins. Indeed Hatakeyama et al.  found a very good correlation between sulfate and ammonium over the East China Sea and concluded that this indicated quick neutralization of sulfuric acid by ammonium in the polluted air mass. Ishizaka and Adhikari  found that CCN compositions at a coastal site of a Japanese main island were dominated by ammonium sulfate. McNaughton et al.  pointed out that hygroscopic growth of 25 nm particles was best explained by an ammonium sulfate/ammonium bisulfate type composition for the Gosan aerosols during ACE-Asia. However, our results are contrary to Dusek et al.  that reported insoluble CCN than our results for the polluted air masses and are also contrary to Hudson and Da , where the authors found that CCN solubility for the air masses under anthropogenic influences tends to be insoluble compared to cleaner air masses.
 Data obtained at a relatively remote coastal site at Gosan in Jeju Island, Korea during the ABC-EAREX 2005 indicates that springtime submicron aerosols were under steady continental influences, regardless of air mass designation. Even the air mass that was the closest to maritime in terms of marine residence time has the average CN and CCN concentrations an order of magnitude higher than those of clean marine boundary layer and were in fact comparable to or even higher than those of marine or coastal environments with significant continental influences.
 Clear sky weather conditions bringing air from northern China, Mongolia or Russia by anticyclonic circulations were found to be a prerequisite for new particle formation and growth at Gosan. Simultaneous occurrence of these events at a western coastal site in the Korean Peninsula 350 km north of Gosan suggests that these events were not local but at least regional-scale events. However, it cannot be verified if the actual formation of new particles occurred near the measurement altitude or new particles were formed aloft and then turbulent mixing took them down to the measurement altitude as the day progressed.
 With the assumption of particles being composed solely of ammonium sulfate, there was a very good agreement between the measured and predicted CCN concentrations based on the measured aerosol number size distributions. The air mass that has the most continental influences showed a slight tendency to overpredict CCN concentrations but the overall agreement is good enough to suggest that springtime Gosan aerosols act almost like ammonium sulfate as far as CCN activity is concerned.
 Lacking in this study were aerosol chemistry analyses, which will be presented by companion papers on aerosol chemistry in this special issue. Combining them with the results of this study would provide a more complete picture of springtime submicron aerosol characteristics at the coastal environment of Gosan, a suitable location to monitor background aerosol distributions in northeast Asia.
 This study is supported by the Korean Ministry of Environment as the Eco-technopia 21 project. The authors want to say special thanks to Soon-Chang Yoon of Seoul National University for allowing them to use his instrument shelter and the aerosol inlet system at the Gosan site.