3.1 CCN number concentrations

The number concentration of CCN at 0.2 % supersaturation, which represents the concentration of aerosols that are hygroscopic and sufficiently large (size >100 nm) to become activated at low (0.2 %) supersaturations, is shown along the cruise track in Fig. 1. High concentrations of CCN (∼2000 cm⁻³) are observed in the plume area (SEAS1), and lower CCN concentrations (<500 cm⁻³) are seen over the southwest part of the cruise track (∼2^∘ S, 65 to 72^∘ E). The low values observed during the return phase of the cruise are attributed to the effective wet scavenging of aerosols due to thunderstorms experienced on 4, 6 and 7 February 2018. The SEAS2 region, which is mostly affected by the advection from the Bay of Bengal region (lying downwind of the Indo-Gangetic Plain; Fig. 1), also showed high CCN concentrations of up to 2500 cm⁻³ indicating the widespread influence of South Asian outflow. The latitudinal gradient of CCN at different supersaturations from 15^∘ N to the Equator, between the longitudes 74 to 75^∘ E, shows distinctly different patterns for the CCN concentrations at low (0.2 %) and high (1.0 %) supersaturations as shown in Fig. 2. At 0.2 % supersaturation, CCN values observed over SEAS1 (1683±435 cm⁻³) are lower or comparable to that over SEAS2 (1868±276 cm⁻³). This is contrary to the CCN values at 1.0 % supersaturation, where CCN values are 2-fold higher over SEAS1 (5954±1493 cm⁻³) compared to SEAS2 (2513±668 cm⁻³). The systematic decrease in the CCN number concentration with latitude is clearly seen below the southern tip (<8^∘ N) of peninsular India, whereas measurements above 8^∘ N are modulated by the heterogeneous sources located along the west coast of India. The CCN concentration at 1.0 % supersaturation was 5- to 7-fold higher than that at 0.2 % supersaturation over SEAS1, whereas the rate of change in CCN concentration with supersaturation is insignificant over SEAS2.

Figure 2Latitudinal variation in the CCN number concentration at 0.2 %, 0.4 % and 1.0 % supersaturations (SS) over the southeastern Arabian Sea (SEAS). The vertical bars on each data point indicate the standard deviation of the measurements. The SEAS region is further divided into SEAS1 and SEAS2 based on the origin of air mass back trajectories and proximity to the mainland.

Download

Figure 3Mean CCN number concentration with the standard deviation at different supersaturations over the northern Indian Ocean (SEAS1, SEAS2 and EIO) during ICARB-2018. The CCN spectra measured at a coastal station, Thumba, are also shown in the figure for comparison. The graph is shown on a log–log scale.

Download

The regional variation in the mean CCN concentration with respect to supersaturation (commonly called CCN spectra) over SEAS1, SEAS2 and EIO is shown in Fig. 3. The mean CCN spectra observed during December 2017 at Thumba (8.5^∘ N, 77^∘ E; Jayachandran et al., 2018), which is located on the west coast of peninsular India (close to SEAS1) and experienced the same synoptic conditions as that during the ICARB-2018 campaign, are also shown in the figure for comparison. In general, the CCN concentration will be higher or remain constant as supersaturation increases. As the set supersaturation inside the instrument increases, more and more particles will become activated since the supersaturation inside the instrument column is higher than the minimum supersaturation (called critical supersaturation) required for the particles to become activated. Hence CCN at higher supersaturation are cumulative, and all particles with critical supersaturation lower than the set supersaturation are activated as CCN. This variation in CCN with supersaturation is parameterized using the Twomey empirical relationship, N_CCN=C  SS^k, where SS is supersaturation and k is the Twomey exponent, which is also mentioned in the figure. Twomey's exponent (k) indicates the qualitative information on the CCN active aerosol size distribution, with high k values implying the dominance of ultrafine-mode aerosols and low k values indicating the fine-mode (>100 nm) aerosol dominance in the measured number size distribution (Fang et al., 2016; Jayachandran et al., 2017; Gunthe et al., 2009). In this study, k values are estimated in the supersaturation range from 0.2 % to 1.0 %. As shown in Fig. 2, the CCN concentration measured in the South Asian outflow is very sensitive to the supersaturation over SEAS1 (coastal regions adjoining India), whereas CCN concentration is less dependent on supersaturation over the regions far away from the continental sources (SEAS2 and EIO). The higher (0.83±0.22) value of Twomey's exponent (k) over SEAS1 (steep CCN spectra) is attributed to the dominance of ultrafine-mode aerosols (or somewhat hydrophobic aerosols) in the continental outflow. The lower k values of 0.21±0.19 and 0.13±0.11 estimated for SEAS2 and EIO respectively suggested larger particle dominance due to the extended transit of aerosols over the oceanic regions leading to enhanced sizes.

It would be interesting to compare the present values of CCN with the previous observations, which are rather scarcely reported over the oceanic regions surrounding South Asia. Based on the shipborne measurements during INDOEX, Cantrell et al. (2000) reported the CCN concentration of 1000 to 2500 cm⁻³ (at 0.5 % supersaturation) over 10 to 15^∘ N. Similarly, airborne measurements on board a research flight (NCAR C-130) during INDOEX reported the values of CCN at 1.0 % supersaturation as ∼1190 cm⁻³ for polluted air masses and less than 176 cm⁻³ for clean marine conditions over the southern Indian Ocean (Hudson and Yum, 2002). The CCN values over the SEAS1 region during ICARB-2018 are (i) higher than the CCN values reported during INDOEX, (ii) comparable to the values at the coastal site (Thumba) in southern peninsular India and (iii) less than the values reported from polluted continental locations in the Indo-Gangetic Plain (Jayachandran et al., 2020). The CCN values observed over SEAS are mostly lower or comparable to the values over polluted continental sites (2900±2800 cm⁻³ at 0.4 % supersaturation) as reported by Andreae (2009) based on the compilation of CCN observations carried out worldwide. Interestingly, the CCN values over EIO (which is the relatively remote oceanic region) during ICARB-2018 are almost 7-fold higher than the clean marine CCN values (107±56 cm⁻³) and lower than the polluted marine conditions (1060±400 cm⁻³) reported by Andreae (2009). Cantrell et al. (2001) also reported high CCN concentrations (in the range of 300 to 1000 cm⁻³) at 0.3 % supersaturation over Kaashidhoo climate observatory over the equatorial Indian Ocean during February–March 1999. The higher concentration of CCN at the Equator and further south of it clearly indicated the widespread influence of continental outflow over this region (Ramanathan et al., 2001).

In general, as we move away from the continental sources, aerosol abundance (AOD, black carbon and total mass concentration) decrease toward the open ocean as reported by several studies over the northern Indian Ocean (Ramanathan et al., 2001; Moorthy et al., 2009; Hudson and Yum, 2002). Similarly, Chylek et al. (2006) have reported a latitudinal decrease in the CCN concentration at 1 % supersaturation from 1850 cm⁻³ at 4^∘ N to 700 cm⁻³ at 0^∘ N over the Indian Ocean during the INDOEX campaign. Hudson and Yum (2002) reported that the influence of pollution outflow from South Asia to the Indian Ocean ceased at 5^∘ S due to the Intertropical Convergence Zone. Over the same latitudinal sector, the rate of decrease in CCN concentration with latitude was lower during ICARB experiment (1.4 times) compared to the INDOEX values, which further highlighted the persistent and widespread impact of continental outflow over the northern Indian Ocean during ICARB-2018. Besides, CCN variation with supersaturation also depicted a latitudinal gradient with high k values over SEAS1 and low values over EIO. It is interesting to note that, irrespective of the large decrease in aerosol loading and change in aerosol microphysical properties over the region, the CCN concentrations at 0.2 % are comparable at all locations (SEAS1, SEAS2 and Thumba) except over EIO (Fig. 3). The high k values are observed at the coastal site, Thumba (Jayachandran et al., 2018) and measurements from Kaashidhoo Climate Observatory (4.97^∘ N, 73.5^∘ E) during INDOEX (Cantrell et al., 2001). Similar to SEAS1, an average k value of 0.8 was reported over the northeast Atlantic by Snider and Brenguier (2000) during the ACE2 campaign. Schmale et al. (2018) also reported a similar finding based on the data collected from several distinct locations in Europe. The low k values observed over the SEAS2 and EIO also could be due to the cloud processing of maritime clouds (Noble and Hudson, 2019; Hudson et al., 2015). Since the k value of the CCN spectrum depends highly on the dominance of the ultrafine particles in the aerosol size distribution and hygroscopicity of the aerosol system, the k values estimated from the CCN measurements for a short range of supersaturations should be interpreted carefully. It should be noted that carbonaceous particles and newly formed ultrafine particles have a low contribution to the CCN concentration and require extremely high supersaturation conditions for the CCN activation (Dusek et al., 2006b; Pierce and Adam, 2007).

3.2 CCN activation efficiency and geometric mean diameter

The fraction of total aerosol concentration (CN) that can act as CCN at a specific supersaturation (CCN(SS)/CN) is termed CCN activation fraction or activation efficiency, which is governed mainly by the number size distribution and composition of the aerosol system (Schmale et al., 2018; Dusek et al., 2006a). The scatter plot between the CN and CCN over SEAS1, SEAS2 and EIO is shown in Fig. 4a, and the colour scale indicates a geometric mean diameter (GMD) corresponding to the composite aerosol number size distribution. CCN being a specific subset of CN, the CCN concentrations increased with increasing total aerosol concentrations during most of the observations. Regression analysis of CN and CCN at 0.4 % (slope ∼0.2 and R² ∼0.45) and 1.0 % (slope ∼0.29 and R²∼0.44) supersaturations has a poor association during the entire campaign period. This is in contrast to the earlier observations (Gunthe et al., 2009; Jayachandran et al., 2018), where the association between CN and CCN increased with supersaturation. When the CN concentration was very high and ultrafine-mode aerosols contributed significantly to the CN concentrations, as evident from the lower values of the GMD of the aerosol size distribution (Fig. 4a, colour scale), a weak association between CCN and CN was observed. For GMD values greater than 100 nm, CCN and CN followed an excellent relationship with R² ∼0.99 and mean activation efficiency of 69±10 % over all the regions (SEAS1, SEAS2 and EIO). This highlighted that most of the particles in this size range become activated as CCN irrespective of the regional heterogeneities in the aerosol composition. As aerosol system having a GMD of less than 60 nm (when ultrafine particles dominate the aerosol size distribution) has deviated significantly from the regression line. This implies that the abundance of ultrafine particles has a direct impact on activation efficiency, since most of these particles may not become activated at 0.4 % and 1.0 % supersaturation levels (Pierce and Adam, 2007).

Figure 4(a) Scatter plot between total aerosol (CN) and CCN at 0.4 % supersaturation over SEAS1, SEAS2 and EIO. The colour shows the geometric mean diameter (GMD) of the aerosol size distribution. Regression fit for a GMD greater than 100 nm is shown as a black dotted line. (b) Temporal variation in CCN concentration at 0.4 % supersaturation (SS) measured using a CCN counter and estimated using the empirical relationship between total aerosol number concentration and geometric mean diameter. The “p” and “n” are empirical constants estimated using the regression technique. The scatter plot of measured and estimated CCN concentration is shown inset.

Download

The influence of the GMD on the CN–CCN association is further investigated using the regression analysis between the observed CCN at 0.4 % supersaturation with the product of CN and GMD (CN ⋅ GMD). The coefficient of determination (R²) had improved from 0.44 to 0.84 when CN is multiplied with the GMD. The CCN concentration is estimated from the empirical relationship between the CN and GMD (CCN${}_{\mathrm{est}}=n\cdot \mathrm{CN}\cdot \mathrm{GMD}$, where n is a constant), which showed an excellent association with the measured CCN concentration (at 0.4 % supersaturation). The regression coefficient between measured and estimated CCN further increased to 0.94 for a power law, CCN${}_{\mathrm{est}}=n\cdot \mathrm{CN}\cdot {\mathrm{GMD}}^p$, where p (1.5) and n (2000) are constants estimated iteratively for the highest value of R². The temporal variation and scatter plot of measured and estimated CCN concentrations at 0.4 % supersaturation are shown in Fig. 4b. By accounting for the effect of the GMD on CCN concentration, this analysis demonstrated the primary role of aerosol number size distribution on CCN activation. Since the ultrafine-mode aerosols have lesser hygroscopicity compared to the fine-mode (>1 µm) aerosols (Pöhlker et al., 2016; Gunthe et al., 2009; Pierce and Adams, 2007; Rose et al., 2011), the empirically estimated CCN number concentration is overestimated during the periods of ultrafine-particle dominance in the size distribution. The low activation efficiencies during the new-particle formation events and for the higher abundance of ultrafine-mode aerosols have been reported in the literature (Pöhlker et al., 2016). The present analysis of estimating the CCN concentration from the product of CN and GMD for widely varying aerosol size distributions is analogous to the better association between the product of the aerosol scattering coefficient and its spectral dependence (Ångström exponent) with CCN concentration rather than the regression between scattering coefficient and CCN concentration (Jayachandran et al., 2018).

In general, aerosol size distribution plays a major role in CCN activation. The ultrafine particles significantly decrease the activation efficiency compared to the fine-mode aerosols. Since the CN number concentration decreased from the southeastern Arabian Sea to the equatorial Indian Ocean, delineating the periods of ultrafine-particle dominance from a threshold CN value is difficult (see Fig. 4a). The CN values over the equatorial Indian Ocean (>5000 cm⁻³) during ultrafine-particle events are lower than the CN values without ultrafine-particle events over the southeastern Arabian Sea region. The association of CCN activation efficiency with the CN number concentration over different regions is shown in Fig. 5. For a constant CN concentration (5000 cm⁻³), the CCN activation efficiency at EIO (∼15 %) is much lower than that of SEAS1 (∼65 %) due to the presence of more ultrafine particles in EIO. Figure 5 highlights that the activation efficiency decreases with CN concentration following power-law dependence (AE $=a\cdot {\mathrm{CN}}^b$, where a and b are constants) with similar coefficients ($b=-\mathrm{0.84}$, R²=0.85) over both SEAS1 and EIO regions. Yum et al. (2007) also showed that CCN efficiency decreases with the increase in ultrafine-particle concentrations irrespective of air mass type, which implies the lower hygroscopicity of these particles (Pierce and Adams, 2007).

Figure 5Association of activation efficiency at 0.4 % supersaturation (SS) with CN number concentration during SEAS1, SEAS2 and EIO of ICARB-2018. Dotted lines indicate regression fit to the data.

Download

The scatter plot between the CCN activation efficiency at 0.4 % supersaturation and the GMD of aerosol size distribution segregated for different marine regions is shown in Fig. 6a. It is clear that the higher CCN activation efficiency is observed for particle size distributions dominated by larger particles (GMD >130 nm) irrespective of the regions and air mass patterns. Wherever the contribution of ultrafine particles to the total aerosol concentration is significant, the activation efficiency decreased. In general, low (high) GMD values resulted in low (high) CCN activation efficiency, irrespective of aerosol composition, in the south Asian outflow. For a given GMD of 90 nm, the activation efficiency varied over a wide range from 20 % to 60 %, which is more notable over the EIO region (stars), where the ultrafine particles contribute 20 % to 50 % to the total number concentrations. Earlier, Kim et al. (2014) also observed a significant spread in the association between CCN at 0.6 % supersaturation and a GMD in the range of 40–70 nm, which is attributed to the heterogeneities in aerosol chemical composition. The association between the GMD and activation efficiency weakened during the new-particle formation events and aerosol size distributions having multiple modes, especially in the coarse- and ultrafine-particle regime. Supersaturation spectra of CCN activation efficiency for low (25–50 nm) and high (125–150 nm) values of the GMD are shown in Fig. 6b. In contrast to SEAS1 and EIO, low-GMD cases were not observed over SEAS2. For low-GMD cases, activation efficiency at 1.0 % supersaturation is mostly less than 30 % over SEAS1 and EIO, which implies the low hygroscopicity of the ultrafine particles. In contrast, higher activation efficiencies (>60 %) are observed for high-GMD cases over all the regions irrespective of the supersaturation conditions. The very low activation efficiency at 0.2 % supersaturation (∼30 %) observed over the SEAS1 region increased drastically to ∼100 % at 1.0 % supersaturation for high-GMD conditions. Regionally, SEAS1 aerosols are more CCN active, especially at higher supersaturations (1.0 %) compared to the EIO aerosols (Fig. 6b).

Figure 6(a) Association of geometric mean diameter (GMD) with CCN activation efficiency at 0.4 % supersaturation (SS) over SEAS1, SEAS2 and EIO during ICARB-2018. (b) Supersaturation spectra of activation efficiency for low (25–50 nm) and high (125–150 nm) GMD values during SEAS1 and EIO. All the size distribution measurements during SEAS2 have a GMD above 50 nm. Vertical bars on the symbol indicate the standard deviation of the measurements.

Download

The above discussions highlighted the significant role of the GMD and, in turn, the abundance of ultrafine aerosols in the activation efficiency of the aerosol system. This analysis broadly confirms the primary role of aerosol size distribution in deciding the CCN concentration and activation efficiency over the region. During ICARB-2018, GMD values varied from 25 to 160 nm, and nearly 40 % of the measurements have a GMD of less than 100 nm. The high activation values are observed whenever the contribution of ultrafine-mode aerosols to the CN is negligible. Also, higher CN values (>10⁴ cm⁻³) with low GMD values (<60 nm) are seen over both the SEAS1 and EIO regions suggesting new-particle formation events. A low CCN efficiency at 0.2 % supersaturation at SEAS1 reinstates the dominance of ultrafine particles or the hydrophobic nature of the particles resulting from the continental outflow. It is well known that bimodal distribution is a characteristic of the aerosol system over the marine environment (one mode emanating from possible nucleation events and the other one in the lower size range of the fine mode), whereas aged continental outflows over the oceans show a unimodal distribution with a mode around 80 to 200 nm (Yum et al., 2007). The measurements of aerosol particle size distributions carried out over the Bay of Bengal during winter 2009 (ICARB-2009) revealed a unimodal size distribution with a mode diameter close to 100 nm. This further supports the lack of ultrafine particles over SEAS2, where air masses mostly originate from the Bay of Bengal. At low supersaturations, marine aerosols have a higher CCN activation efficiency compared to the continentally influenced aerosol system, which flip-flops at higher supersaturations. This aspect is further investigated using the aerosol size distribution and critical diameter in the following section. The present study is also in line with the earlier observations reported over various oceanic regions, which depicted a higher activation efficiency for continental aerosols than clean marine aerosols (Yum et al., 2007). A strong association is observed between the GMD and a hygroscopicity parameter for different mixing state conditions (external, internal and internal with non-growth) over the Korean peninsula (Kim et al., 2018). The present study highlight that the higher activation efficiencies are observed for the continental or marine aerosols mostly in the absence of ultrafine-particle burst events.

3.3 Aerosol size distribution and CCN activation

To understand the effect of ultrafine particles on CCN activation, two typical cases have been considered over SEAS1 and EIO, where aerosol size distribution varied drastically within a few hours due to ultrafine-particle events which are characterized by low GMD values and a high number concentration of ultrafine particles (diameters <100 nm). Figure 7 shows the CCN spectra and activation efficiency along with the corresponding aerosol number size distribution over SEAS1 and EIO for high and low concentrations of ultrafine particles (high UFP and low UFP). Corresponding k values (Twomey's empirical slope) are also mentioned in the figure. Over SEAS1, the variation in CCN with supersaturation for high- and low-UFP cases showed an almost similar pattern with a relatively steeper increase in CCN with supersaturation for high UFP compared to low UFP. The CCN activation efficiency for low-UFP case increased from ∼33 % at 0.2 % supersaturation to almost 100 % at 1.0 % supersaturation, whereas for high UFP the activation efficiency at the highest supersaturation (1.0 %) is only ∼45 % over SEAS1. This significant difference in the activation efficiency for the two cases can mostly be attributed to the higher concentrations of ultrafine particles, as already mentioned in the earlier section and Fig. 7b. The particles below 100 nm contributed almost 37 % to the total number concentration for the low-UFP case, and all these particles are activated at high supersaturation in contrast to the high-UFP case. The large amounts of ultrafine-particle concentrations (with a GMD of ∼50 nm in Fig. 7b) seen in the high-UFP case did not contribute significantly to the CCN concentrations even at 1.0 % supersaturation.

Figure 7(a, c) Typical cases of supersaturation spectra of CCN number concentration and activation efficiency (AE) for high and low concentration of ultrafine particles (UFP) over SEAS1 and EIO. (b, d) The aerosol number size distributions corresponding to (a) and (c).

Download

Over EIO, though the CCN values at lower supersaturations are comparable for both the cases, a 100 % increase is observed in CCN concentration at 1.0 % supersaturation for high UFP compared to low UFP (Fig. 7c). The activation efficiency depicted an entirely distinct pattern with low values (20 %) at all supersaturations for high UFP compared to the activation efficiency of >75 % for the low-UFP case. These typical events over SEAS1 and EIO clearly demonstrate the lower activation efficiency of ultrafine aerosols. However, there exist strong differences in the activation properties of CCN over SEAS1 and EIO. For both high- and low-UFP cases, SEAS1 aerosols are more CCN active at higher supersaturations than EIO, which is also clearly reflected in the regional mean values. The absolute magnitude of CCN concentration is relatively less over EIO with no significant increase in CCN concentration with increasing supersaturation (especially for low UFP, k∼0.05). These flat CCN spectra (lower k values <0.5 in both the cases) observed over EIO represent maritime aerosol. The high k values (>0.8) over SEAS1 represent polluted marine conditions (Jayachandran et al., 2017). The aerosol system can have a high and low activation efficiency or k depending on the contribution of ultrafine-mode aerosols to the total number concentration. This is contrary to the general classification of the aerosol system based on k (Jayachandran et al., 2017). The inverse relationship between the Twomey exponent (k) and activation efficiency reported by Jayachandran et al. (2017) over coastal-location Thumba, which is geographically closer to SEAS1, does not hold during ICARB-2018 because of the new-particle formation events and the abundance of ultrafine particles. This is similar to high-UFP cases, as shown in Fig. 7.

To evaluate the relative importance of aerosol number size distribution in CCN activation, similar aerosol size distributions are grouped by regressing each individual size distribution with all the other size distributions. The size distribution having the maximum number of occurrences of the coefficient of determination (R²) greater than 0.9 is identified as the first group. Then, the first group of distributions are removed, and regression analysis is repeated to estimate the next major prominent size distribution (Fig. 8a). The mean number size distributions and corresponding mean activation efficiency at 0.4 % supersaturation for each of the groups are shown in Fig. 8b. This analysis highlighted that the majority of the hourly mean size distributions (number N∼119) depicted a broad peak with the mode around 150–300 nm (Type 1) with the highest activation ratio of 76 %. Whenever the mode of the size distribution falls below 100 nm, i.e., the mode is in the ultrafine-particle regime (Type 2, Type 5 and Type 6), a lower activation efficiency of value below 20 % was observed. The Type 3 and Type 4 size distributions, which are similar to Type 1 but with a small difference in the particle concentration above 100 nm, also showed a higher activation efficiency (>70 %). The spread seen in activation efficiency (standard deviation) for a “fixed” aerosol size distribution could be due to the difference in aerosol chemical composition. It should be kept in mind that, even though we grouped the similar distributions (R²>0.9), the small variations observed between the member distributions (standard deviation of size distributions shown in Fig. 8a) can also contribute to the standard deviation of the activation efficiency. The difference between the activation efficiencies for two distinct size distributions is more substantial than their standard deviations, which initially implies the primary role of number size distribution on the CCN activation.

Figure 8(a) Most frequently occurring aerosol number size distributions (normalized) during ICARB-2018. Vertical bars represent the standard deviation of the data, and the number of hourly observations averaged for each distribution is given in (b). (b) Activation efficiency at 0.4 % supersaturation of the normalized distributions shown in panel (a).

Download

We have further examined the association of CCN concentration with aerosol number concentration (dN) at different size ranges. Figure 9a shows the scatter plot of CCN concentration with the cumulative aerosol number concentration above the size range of 50 nm (N₅₀), 100 nm (N₁₀₀) and 150 nm (N₁₅₀). The slope of the regression fit and coefficients of determination (R²) estimated for the CCN and aerosol concentrations above different size ranges (up to N₂₅₀) are shown in Fig. 9b. The slope of the regression analysis increased as the lower size cut of the aerosol number concentration increased from 50 to 250 nm. The coefficient of determination (R²) was low for N₅₀ and increased to 0.98 for N₁₀₀. The CCN varied with CN concentration where the slope of the variation strongly depended on the size distribution and is stronger for larger aerosols (GMD values >100 nm as shown in Fig. 4) and weaker for ultrafine-mode aerosols. The scatter between CCN at 0.4 % supersaturation and CN₁₀₀ shows better association (slope ∼0.95 and R²∼0.92). This implies that most of the particles above 100 nm are CCN at 0.4 % supersaturation and N₁₀₀ is a good proxy for CCN concentration at 0.4 % supersaturation. The contribution of particles to the CCN concentration at 0.4 % supersaturation is lower above 100 nm. For the particles above 200 nm, CCN concentration is nearly 2.5 times higher than the N₂₀₀.

Figure 9(a) Scatter plot between CCN number concentrations at 0.4 % supersaturation (SS) with aerosol number concentration (CN) for particles size larger than 50, 100 and 150 nm. (b) Variation in regression coefficients (slope and R²) estimated for CCN at 0.4 % supersaturation with aerosol number concentration at different size ranges. The N₅₀ indicate aerosol number concentration above 50 nm.

Download

The above analysis indicates that the critical activation diameter, which is the size above which all the aerosols become activated as CCN (at 0.4 % supersaturation) is close to 100 nm for the continental outflow of aerosols to the northern Indian Ocean during wintertime. The critical activation diameter of the aerosol system can be experimentally estimated from size-segregated CCN measurements (Rose et al., 2010) or from the simultaneous observations of CCN and aerosol number size distributions (Furutani et al., 2008). Assuming an internally mixed aerosol system, we have estimated the “apparent critical diameter” for a particular supersaturation by integrating the aerosol number concentration (dN) from a higher to a lower size range in such way that estimated aerosol number concentration equals CCN concentration (Burkart et al., 2011) and the diameter corresponding to that is called the critical diameter. The cumulative number concentration (summing from higher size to lower) and critical diameter for different supersaturations over SEAS1, SEAS2 and EIO are shown in Fig. 10a and b. As seen in Fig. 10a, the contribution of ultrafine particles to the total concentration is relatively high over SEAS1 compared to SEAS2 and EIO due to the continental proximity. As expected, the critical diameter was lower for higher supersaturations for all the regions. This is consistent with the Kohler theory. A relatively large decrease in critical diameter with supersaturation was observed over SEAS1 compared to SEAS2 and EIO. As shown in Fig. 2, though the aerosol loading is high over SEAS1, CCN concentration at 0.2 % supersaturation is lower over SEAS1 compared to that of EIO. The high value of the critical diameter (∼185 nm) over SEAS1 further confirms that only a small portion of the aerosol population is activated as CCN at 0.2 % supersaturation. This is mostly attributed to the presence of less hygroscopic aerosols (possibly carbonaceous) above 100 nm size range, which requires higher supersaturation to become activated. In contrast, the lower critical diameter at 1.0 % supersaturation over SEAS1 could be attributed to the water-soluble aerosol in the ultrafine-particle mode. It is interesting to note that the critical diameter at 1.0 % supersaturation is higher for EIO than SEAS1 in contrast with 0.2 % and 0.4 % supersaturations. This observation is in line with the high activation efficiency at 1.0 % supersaturation over SEAS1 compared to EIO (Fig. 6).

Figure 10(a) Cumulative aerosol number concentration from higher size range to lower over SEAS1, SEAS2 and EIO. The value at 9 nm indicates the total number concentration. The apparent critical activation diameter is shown as dashed vertical lines. (b) Variation in critical diameter for 0.2 %, 0.4 % and 1.0 % supersaturations (SS) over SEAS1, SEAS2 and EIO.

Download

Simultaneous measurements of aerosol number size distribution and CCN at different supersaturation are useful in understanding CCN characteristics. The size distribution over SEAS1 has a mode close to 100 nm, which represents the influence of polluted continental air mass. Ueda et al. (2016) reported bimodal size distributions as a typical maritime aerosol system based on the extensive measurements of aerosol number size distributions over the Pacific Ocean covering 40^∘ N to 40^∘ S. However, most of the measurements during ICARB-2018 depicted broad mono-modal distribution indicating the aged, continental outflow aerosols. The bimodal distributions are less frequent and mostly associated with ultrafine-particle bursts (Fig. 8). A fine mode has been consistently present in the aerosol number size distribution over SEAS, which is contributing to the high CCN activation. The regional difference in the aerosol number size distribution and its role in determining the activation efficiency of CCN are vivid such that the dominance of fine or ultrafine particles decreases the CCN efficiency from the expected values. Kalivitis et al. (2015) investigated the association of CCN at 0.2 % supersaturation with aerosol concentrations larger than the threshold diameter (from 80 to 130 nm) over the eastern Mediterranean marine atmospheric boundary layer. These authors reported particle concentrations above 100 nm as the best indicator for CCN at 0.2 % supersaturation over the region, and the present study supports this finding (Fig. 9). Burkart et al. (2011) attributed the high critical diameter of aerosols at 0.5 % supersaturation over Vienna to the presence of insoluble aerosols. Rose et al. (2010) have reported a dry activation diameter of 200 to 30 nm for a wide range of supersaturations of 0.068 % to 1.27 %.

The presence of significant amounts of ultrafine particles observed over the northern Indian Ocean could be attributed to the in situ new-particle formation events and/or transport from the free troposphere. The ICARB-2018 measurements indicate that these ultrafine-particle events are mostly observed during the early morning and evening hours. A nearly 20 % to 40 % increase in the mass concentration of organic carbon (OC) was observed during such conditions, implying the formation of secondary organic aerosols. A large-scale anticyclonic system prevailed during the wintertime over the region and also supported the amalgamation of distinct air masses and intrusion of ultrafine particles formed in the free troposphere into the lower atmosphere. The absence of a very high concentration of nucleation aerosols (<10 nm) further confirms the possibility of the transport of free-tropospheric aerosols. Nair et al. (2013) have reported ultrafine-particle dominance over the northern Arabian Sea during spring 2006, which was strongly associated with the variation in chlorophyll concentrations implying a role of ocean biogeochemistry. However, the role of ocean biogeochemistry and that of the semi-volatile organic vapours in the formation of ultrafine particles over the northern Indian Ocean needs to be investigated in detail.

Since the CCN activity depends mainly on the aerosol size and composition (Dusek et al., 2006a), the critical diameter can be regarded as a proxy for the variations in the chemical composition of the aerosol system. It should be emphasized that the aerosol size distribution and chemical composition are intrinsically coupled with each other, and any change in the aerosol size distribution may have also been due to aerosol composition differences. Quinn et al. (2008) have correlated the critical diameter with the hydrogenated organics aerosol (HOA) mass concentration and found that HOA can explain about 40 % of the variance in the critical diameter. For anthropogenic and marine environments, Furutani et al. (2008) have reported a critical diameter of 70–110 and 50–60 nm respectively at 0.6 % supersaturation. The critical diameter estimated for the South Asian outflow is comparable to the values of 70–90 nm (at 0.44 % supersaturation) reported by Quinn et al. (2008) for marine regions. It should be noted that the freshly emitted carbonaceous combustion particles have a high critical diameter (∼350 nm) even at a high supersaturation (0.7 %) as reported by Dusek et al. (2006b). The presence of soluble aerosols largely enhances the CCN activity of insoluble particles such as BC and dust (Dusek et al., 2006b) due to effective mixing. Thus, these inferences underline the need for observations of mixing state that are more realistic and size-segregated aerosol composition measurements in regions like SEAS, where primary as well as secondary particles are present from both natural and anthropogenic sources.

This study highlighted the high concentration of CCN over the South Asian outflow regions. The relative importance of aerosol size distribution and chemical composition in CCN activation has been the topic of investigation for several experiments (Dusek et al., 2006a; Kerminan et al., 2012; Hudson, 2007). A significant understanding of the critical diameter (Kerminan et al., 2012) and size-segregated hygroscopicity parameter (κ) (Petters and Kreidenweis, 2007) enabled us to predict the CCN concentration based on the measurement of physical and chemical properties of aerosols carried out at distinct environments (Schmale et al., 2018). Paramonov et al. (2015) have shown that the hygroscopicity parameter decreases with particle size, with the ultrafine- and fine-mode aerosols having a statistically significant difference in hygroscopicity values. Our observations with the lower activation efficiency observed for distributions with ultrafine-particle dominance agree with Paramonov et al. (2015). Several studies have considered an average size distribution of aerosols with a varying hygroscopicity parameter to predict CCN concentration (Rose et al., 2010; Gunthe et al., 2009; Jurányi et al., 2010). These studies also emphasized that aerosol size distribution has a major role in deciding the number concentration of CCN. Meng et al. (2014) reported that hygroscopicity is more critical at low supersaturations and not at high supersaturations. While the present study described the CCN characteristics over the different parts of the northern Indian Ocean and its association with particle number size distributions, further studies are required to examine the climate implications of these observations.