Long-Term Variation of Black Carbon Absorption Aerosol Optical Depth from AERONET Data over East Asia

: Absorption aerosol optical depth induced by black carbon (AAOD BC ) was retrieved using the depolarization ratio and single scattering albedo provided by the Aerosol Robotic Network (AERONET) inversion products over East Asia. Our analysis considered AERONET data from six sites in East Asia that are mostly a ﬀ ected by anthropogenic pollution, black carbon (BC) emissions, and natural mineral dust, during the period 2001–2018. We identiﬁed a rapid reduction in total aerosol optical depth (AOD T ) of − 0.0106 yr − 1 over Beijing, whereas no considerable trend was observed at the Korean and Japanese sites. The long-term data for AAOD BC showed decreasing trends at all sites. We conclude that successful emission control policies were the major underlying driver of AOD T and AAOD BC reductions over East Asia, particularly in China, during the study period. Values of the AAOD BC / AOD T ratio revealed that, although these policies were successful, the Chinese government needs to undertake stricter measures toward reducing BC emissions. We found that AAOD BC follows seasonal trends, peaking in the colder months. This suggests that in East Asia, particularly in China, domestic coal burning is still of concern.


Introduction
Atmospheric aerosols can greatly affect the global climate by scattering and absorbing solar radiation and influencing cloud formation [1,2]. Population growth, urbanization, and economic development have considerably increased anthropogenic emissions of aerosols [3]. The incomplete combustion of fossil fuels, biomass, and carbon-containing substances emits black carbon (BC) aerosol particles, particularly in developing regions such as East Asia [4], which is one of the main source regions of not only BC and other anthropogenic pollutants, but also natural mineral dust [5][6][7]. China, in particular, is a major source of BC because of its large population and high fossil fuel consumption [8]. Indirect effects of BC include changing the microphysical properties of clouds, and its direct effects include temperature increase through light absorption [9][10][11]. High atmospheric aerosol levels over East Asia, including BC, affect not only local air quality but also the radiative balance of downwind areas [12]. Despite the availability of global atmospheric aerosol information, there is little data observed for more than 10 years available for BC concentrations in East Asia. Furthermore, there is no record of the impact of BC's light-absorption on aerosol optical depth (AOD) and its trends over time. The Aerosol Robotic Network (AERONET) is a global network of ground-based sun/sky photometers that provide long term data on aerosols, such as depolarization ratio (DPR), spectral AOD, Remote Sens. 2020, 12, 3551 2 of 17 column single scattering albedo (SSA), particle size distribution, and absorption AOD (AAOD). Overall, AAOD defines the column aerosol loading of light-absorbing particles such as BC, carbon-containing particles, or mineral dust. Calculation of AAOD is complicated when different types of absorbing aerosol are present in a mixed aerosol plume.
Because BC is the main light absorber in the atmosphere, and also affects atmospheric chemical processes and air quality, the quantification of its specific AAOD (AAOD BC ) is critical [13]. Although several studies have investigated the contribution of BC to aerosol light absorption from AERONET columnar observations [14], few studies have determined AAOD BC and its optical properties. Schuster et al. [15] derived the BC concentrations and the specific absorption from AERONET measurements to describe the radiance field and absorption optical thickness. Russell et al. [13] applied SSA, absorption Ångström exponent, and AAOD from AERONET data to identify the individual shares of BC, mineral dust, and organic matter in the total AAOD. Shin et al. [14] discussed the contribution of BC-related absorption to the non-dust AAOD. To the best of our knowledge, this is the first study in which the contribution of AAOD BC to the total AOD has been studied over a period of 18 years in East Asia.
In this study, we retrieved the AAOD BC from AERONET version 3 level 2.0 data using DPR and SSA to identify its long-term trends and seasonal variations in East Asia. The work is beneficial to the analysis of areas of (and downwind of) deserts with notable contributions of dust to AAOD. Section 2 describes our methodology; Section 3 provides the results; Section 4 describes the discussion; Section 5 presents a summary and conclusion of this study.

AERONET Version 3 Data and Sites
AERONET sun/sky radiometers measure direct solar and sky radiation. The measurements are analyzed automatically by the AERONET inversion algorithm [16,17]. All AERONET data are stored in an online database (http://aeronet.gsfc.nasa.gov, AERONET, 2019) and the measurements are downloadable. AERONET instruments measure AOD at 440, 670, 870, and 1020 nm. In the absence of cloud contamination, the AOD uncertainty is estimated as 0.01 to 0.02 depending on wavelength. Additionally, the calibrated sky radiance measurements have uncertainties below 5%. AERONET inversion code provides aerosol optical properties in the total atmospheric column derived from the direct and diffuse radiation measured by AERONET sun/sky radiometers. AERONET version 3 level 2.0 inversion products provide DPRs at 440, 675, 870, and 1020 nm as well as AOD and other properties such as SSA. In addition, the outputs of inversion products provide estimates for random and possible systematic errors resulted from possible biases in measurements for most of the retrieved characteristics. SSA is used to determine the share of scattered light and the fraction of AOD related to light absorption (i.e., AAOD). The uncertainty in SSA was reported to be of the order of 0.03 [16].
This study selected AERONET sites with the following considerations. First, the sites must measure the optical properties of atmospheric aerosols generated in East Asia. Second, they must show variations in aerosol optical characteristics due to the mixing of dust and anthropogenic aerosol during long-range transport. Third, the sites should be able to provide long-term data on the variations in optical properties for at least 10 years. Figure 1 shows  . Urbanization and industrialization in East Asia, specifically in China, have led to a vast emission of anthropogenic aerosols in this region. East Asian dust storms originating in the Asian desert also raise dust particles into the atmosphere. Readings at the selected sites are influenced by both anthropogenic (e.g., those from fossil fuels and biomass burning) and natural (e.g., mineral dust) aerosols [18]. The AERONET inversion algorithm is only performed for observations with AODs larger than 0.4 at 440 nm [17]. In this study, the data on particle linear DPR (PLDR), SSA, and size distribution is derived from the AERONET (level 2.0 (quality-assured), version
Previous researchers have found that the DPR measured by LIDAR can be used to distinguish between dust and pollution (non-dust) particles [28][29][30]. Noh et al. [31] confirmed that the DPR at 532 nm measured by LIDAR, and that at 1020 nm retrieved from AERONET data, were highly correlated. Therefore, we applied the method of Shin et al. [14] to separate dust and non-dust particles using the DPR at 1020 nm from AERONET data, and consequently calculate AAODBC using only the SSA of pollution particles.
The particle linear DPR can be used as a parameter to obtain insight into the variation of optical and microphysical properties of particles. The AERONET version 3 level 2.0 inversion product provides particle linear DPRs ( ) at 440, 675, 870, and 1020 nm. Shin et al. [32] showed that any value of at 1020 nm greater than 0.30 represents pure Asian dust particles, while values below 0.02 indicate Asian anthropogenic pollution particles [33]. Values between these two thresholds (labeled and , respectively) represent a mixture of dust and other aerosols such as anthropogenic pollution and non-dust particles. Therefore, the can be used to distinguish the share of pure dust and nondust in a mixed plume [14,29]. The dust ratio (Rd) was first calculated here using values at 1020 nm from AERONET data. Shimizu et al. (2004) gave the following calculation for Rd [28]: Rd = (2) Noh et al. [31] concluded that the high correlation of at 1020 nm from AERONET version 3 inversion data, and that from LIDAR measurements, means that the AERONET data can be used to assess the presence of dust particles. The value of Rd allows the total AOD (AODT) at 1020 nm to be separated into components for dust (AODD) and non-dust (AODnd): AODD,1020 = AODT,1020 × Rd,1020

AAOD BC Retrieval Methodology
Most aerosols in the atmosphere scatter light and absorb it in different levels, but BC has a strong light absorbing ability [19][20][21][22], as do dust particles [23][24][25][26][27]. In the absence of dust particles, BC is mainly responsible for the light absorbed by atmospheric aerosols, and BC's specific AAOD (AAOD BC ) can be calculated simply from the SSA: where, λ indicates wavelength. However, in the presence of dust particles, their effect must be separated to calculate AAOD BC . Previous researchers have found that the DPR measured by LIDAR can be used to distinguish between dust and pollution (non-dust) particles [28][29][30]. Noh et al. [31] confirmed that the DPR at 532 nm measured by LIDAR, and that at 1020 nm retrieved from AERONET data, were highly correlated. Therefore, we applied the method of Shin et al. [14] to separate dust and non-dust particles using the DPR at 1020 nm from AERONET data, and consequently calculate AAOD BC using only the SSA of pollution particles.
The particle linear DPR can be used as a parameter to obtain insight into the variation of optical and microphysical properties of particles. The AERONET version 3 level 2.0 inversion product provides particle linear DPRs (δ p ) at 440, 675, 870, and 1020 nm. Shin et al. [32] showed that any value of δ p at 1020 nm greater than 0.30 represents pure Asian dust particles, while values below 0.02 indicate Asian anthropogenic pollution particles [33]. Values between these two thresholds (labeled δ p d and δ p nd , respectively) represent a mixture of dust and other aerosols such as anthropogenic pollution and non-dust particles. Therefore, the δ p can be used to distinguish the share of pure dust and non-dust in a mixed plume [14,29]. The dust ratio (R d ) was first calculated here using δ p values at 1020 nm from AERONET data. Shimizu et al. (2004) gave the following calculation for R d [28]: Noh et al. [31] concluded that the high correlation of δ p at 1020 nm from AERONET version 3 inversion data, and that from LIDAR measurements, means that the AERONET data can be used to Remote Sens. 2020, 12, 3551 4 of 17 assess the presence of dust particles. The value of R d allows the total AOD (AOD T ) at 1020 nm to be separated into components for dust (AOD D ) and non-dust (AOD nd ): where the subscript numbers denote the wavelength in nm. To convert AOD D,1020 to corresponding values for other wavelengths, we used the Ångström exponent of pure Asian dust (å D = 0.14) [30]: which can be used to calculate AOD nd,λ : Dark mineral phases like iron oxides influence the visible-light absorption of mineral dust [34][35][36], while BC is the main anthropogenic light absorber across the entire solar spectrum, especially in the mid-visible range [37,38]. The SSA spectral curvature can provide further information on the composition of aerosol mixtures. The SSA increases with increasing wavelength for pure mineral dust, but decreases for anthropogenic pollution or carbon-containing particles [39]. As dust and BC both absorb light in the visible range (around 440 nm), the total SSA (SSA T ) can be split into components for dust (SSA D ) and non-dust (SSA nd ) as follows: where SSA nd is derived as The spectral SSA values for pure Asian dust particles at 440, 675, 870, and 1020 nm have been calculated as 0.94, 0.98, 0.98, and 0.98, respectively, using data for a source region of Asian dust; Dunhuang in Western China (40.49 • N 94.95 • E) [31].
From SSA nd , the share of light scattered by coarse and fine non-dust particles, the non-dust AAOD can be found: Since aerosol light absorption in the atmosphere is dominated by BC, we assume that in the absence of dust particles the light absorption by pollution (non-dust) is mostly due to BC. As BC is not an ideal light absorber, its SSA is not equal to 0. To estimate the BC-related AAOD (AAOD BC ) we used the SSA of BC (SSA BC,λ ): The SSA of fresh BC has been reported as between 0.07 and 0.28 [40][41][42]. Values of 0.25, 0.17, 0.13, and 0.07 were used here at 440, 675, 870, and 1020 nm, respectively.
In the results section, the mean values of our findings and the specific trends for each variation are

Statistical Analysis
To the better interpretation of the AAODBC trends, the average data points for each year at all sites were subjected to a one-way ANOVA test using SPSS statistics application (IBM SPSS Statistics, USA) to compare means at P < 0.05. Table 1 summarizes the daily mean values of total and seasonal variation of AODT, AAODBC,

Statistical Analysis
To the better interpretation of the AAOD BC trends, the average data points for each year at all sites were subjected to a one-way ANOVA test using SPSS statistics application (IBM SPSS Statistics, USA) to compare means at p < 0.05. Table 1 summarizes the daily mean values of total and seasonal variation of AOD T , AAOD BC , and AAOD BC ratio (the ratio of AAOD BC /AOD T , i.e., AOD > 0.4) at 440 nm for the six selected stations over the period 2001-2018.

Total Aerosol Optical Depth (AOD T ) and AAOD BC
The highest values of AOD T in Table 1 are for Beijing, whereas the Japanese sites showed the lowest (almost half those for Beijing). Considering seasonal variation, AOD T was highest in summer at most sites, but not at Anmyeon and Gosan where it was higher in winter and fall, respectively. Beijing showed the highest total AAOD BC and AAOD BC ratio during all seasons, with values greatest in winter. All the Korean and Japanese sites showed roughly similar values of AAOD BC (0.02-0.04), which were clearly less than those for Beijing (0.09-0.13). Figure 2 shows the 18-year (2001-2018) variations of the annual mean AOD T at 440 nm for each site. Beijing showed steeply declining values (−0.0106 AOD T yr −1 ) during the study period, whereas no considerable trends emerged for the Korean and Japanese sites, which showed annual variations between −0.0003 and 0.0027 AOD T yr −1 . Overall, there is some seasonal variability in AOD, which is generally highest in summer (see Table 1). Figure 3 presents the annual variation in AAOD BC at the six sites. Similar to AOD T in Figure 2, Beijing showed the highest annual mean AAOD BC , which was approximately double that at each of the Korean and Japanese sites. Unlike the annual variation of AOD T , AAOD BC declined annually, not only in Beijing but at all sites, with the greatest annual decline (−0.0030 AAOD BC yr −1 ) observed at Osaka. The next greatest annual decline of −0.0026 AAOD BC yr −1 was at Beijing, where the highest AAOD BC of approximately 0.14 in 2002 declined to 0.09 in 2017. The annual mean AAOD BC at Osaka, Shirahama, and Gosan peaked in 2003. The lack of continuous observations at the Korean sites prevented observation of any coherent trend for AAOD BC , but AAOD BC declined overall at these sites from 2001 to 2018. Figure 4 shows the time series of seasonal mean AAOD BC and its trends for the six sites. There is a distinct seasonal trend, with higher values in winter and lower values in summer. Most sites showed annual decreases of AAOD BC ; the exceptions, Anmyeon and Gwangju, showed increases in winter values of 0.0015 and 0.0006 AAOD BC yr −1 , respectively.

BC Ratio
The variations of the annual ratios of AAOD BC to AOD T and AAOD BC to AOD nd at 440 nm and their trends for 2001-2018 are shown in Figure 5a,b, respectively. Both ratios show a long-term declining trend at all sites. As mentioned in Section 3.1, Beijing showed the greatest declining trend for the annual variation of AOD T and the second greatest for AAOD BC (after Osaka), with annual declines of −0.0106 and −0.0026 yr −1 , respectively (Figures 2 and 3). The results in Figure 5 show that Beijing had the smallest decreases in the annual ratios of both AAOD BC /AOD T (after Gosan and Anmyeon) and AAOD BC /AOD nd from 2001 to 2018. Therefore, although Beijing had sharp drops in AAOD BC and AOD T , its ratios of AAOD BC /AOD T and AAOD BC /AOD nd decreased only slightly. On the other hand, for the Korean and Japanese sites, although AOD T remained largely steady, and decreases (in Osaka and Gwangju) were less than those in Beijing, rapid decreases in AAOD BC led the annual ratios of AAOD BC /AOD T and AAOD BC /AOD nd to fall more quickly than those for Beijing. Figure 6 compares the seasonal variation of the annual AAOD BC /AOD T ratio (BC ratio) at 440 nm. It was higher during winter, and lower in summer (below 0.12) at all sites. The observed variation indicates a larger contribution of BC to AAOD in fall and winter. The BC ratio declined at all sites, other than Anmyeon (during spring and winter). The greatest rate of decrease at −0.0100 was at Osaka in the winter.

Statistical Analysis Results
Since AAODBC trends are the main findings of this study, a one-way ANOVA test was applied The monthly mean variations of the ratio of AAOD BC to AOD nd at the six sites are shown in Figure 7c. For Beijing, this ratio increased sharply from October to February, and was lowest in late summer (August).

Statistical Analysis Results
Since AAOD BC trends are the main findings of this study, a one-way ANOVA test was applied to the average data sets at all six sites to further test that if the trends are statistically significant or not. Table 2 summarizes the statistical results of the One-way ANOVA. Among all the selected sites, Beijing and Anmyeon with the p-values of 0.128 and 0.358 did not show a significant difference between the average data points.

Discussion
According to Figure 2, Beijing showed steeply declining values of AOD T during the study period, whereas no considerable trends were found for the Korean and Japanese sites. Yu et al. [43] and Kim et al. [44] reported similar seasonal variations of AOD in Beijing and Gosan, respectively. The higher values and high declining trend of AOD in China have been reported previously [45][46][47]. Yu et al. [48] compared AOD values in East Asia during 2001-2005, and found higher values at Chinese sites than at Korean or Japanese sites. Khan et al. [49] reported a decreasing trend in AOD at 440 nm over the North China Plain, with Beijing showing the highest values from 2001 to 2018; however, some studies have reported that the annual mean AOD has remained constant or increased over Northeast Asia and China [50][51][52]. Nam et al. [50] found the highest annual mean AOD at North China sites and lower values at Korean and Japanese sites. A significantly increasing trend in AOD has been found in North and Northeast China, but no significant trends were identified at sites in Korea (Gwangju) and Japan (Shirahama and Osaka) between 2004 and 2015.
The higher AODs in China and its downwind regions during spring are attributed to dust plumes transported from deserts in Mongolia and China, which coincide with increasing local sources during this season [53,54]. In summer, AOD peaks at most sites due to increased moisture and enhanced formation of secondary aerosols [55][56][57]. Beijing's higher annual mean AOD in comparison to other sites is mainly due industrial pollution and its combination with mineral dust and other anthropogenic particles [58]. This is also associated with high emissions of different chemical species, such as burning fossil fuel (including coal) for transportation, industry, and domestic heating during cold seasons [59]. Furthermore, the declining trend of AOD in Beijing can be explained by improving air pollution control measures and the implementation of strict governmental policies on air pollution [60,61]. The lower variation of annual mean AOD at Korean and Japanese sites is attributable to lower air pollution emissions in comparison to China. The lack of continuous observations and limited data for the Korean and Japanese sites is another possible reason for their lower AOD values.
In Figure 3, Beijing showed the highest annual mean AAOD BC ; besides, AAOD BC declined overall at the Korean and Japanese sites from 2001 to 2018. The trends for Anmyeon and Beijing are not statistically significant; however, the higher values of AAOD BC were found in the Beijing site.
This non-significant trend can result from the higher emissions of BC over China. In the case of the Anmyeon site, the non-significant trend might be due to the few observations and insufficient data sets over this site. Sun et al. [62] found decreasing trends in both AAOD BC and AOD from 2008 to 2017 in China. The variation of AAOD in China from 1980 to 2017 was mostly attributed to the variation of AAOD BC . Other studies have also reported declining trends of BC concentration in Beijing, which may explain the declining trend of AAOD BC in this region [8,21]. The reduction of BC emissions in China appears to result from governmental clean air actions (e.g., Regional Emission inventory in Asia (REAS) version 3.1 and Multi-resolution Emission Inventory version 1.3 (MEIC1.3)), reduction of coal combustion (both industrial and residential), traffic limitation, and gasoline consumption restrictions [63].
Cho et al. [64] compared the contribution of BC to carbonaceous aerosol AAOD at background sites (Gosan, Anmyeon, Shiraham, Fukuoka, and Baengnyeong) and polluted urban regions (Beijing, Gwangju, Osaka, Xianghe, Xuzhou, Taihu, Hongkong, Seoul, and Chiba). They found that BC made a greater contribution to carbonaceous aerosol AAOD in polluted urban regions than in the background cities. Our study found the highest annual mean AAOD BC in China, the largest source of BC in East Asia [65,66]. Liquid fuels such as kerosene, gasoline, and diesel have been found to contribute significantly to BC pollution in Beijing in recent years [67]. The high AAOD BC in China is mainly due to carbon-containing pollutants emitted from industry and other human activities associated with the country's growing economy and population density over the last three decades. Transportation also accounts for significant emissions of BC in Beijing and the neighboring regions. We found lower values of AAOD BC in rural and coastal regions, such as Anmyeon, Gosan, and Shirahama, compared with metropolitan cities such as Beijing, Osaka, and Gwangju. This is related to lower BC emissions from diesel engines for transportation, industrial, and residential use.
According to Figure 4, there is a distinct seasonal trend for AAOD BC , with higher values in winter and lower values in summer. The BC emissions from residential heating accounted for the generally higher winter values of AAOD BC . The highest mean AAOD BC (approximately 0.17) was observed at Beijing in winter 2002; this value had dropped to 0.05 by summer 2016. The mean values in Korea and Japan were consistently lower (less than 0.10) than those observed in China over all seasons. Several studies have reported similar seasonal trends of BC concentrations (lowest in summer, highest in winter) at Chinese sites [68,69]. Zhuang et al. [70] found considerable seasonal variations in BC emissions over East Asia, predominantly driven by changing domestic and residential emissions. Kang et al. [71] attributed increased AAOD over the North China Plain and the Korean Peninsula during winter to seasonal increases of BC and organic carbon (OC) emissions. Incomplete combustion of fossil fuel for domestic heating is a significant source of BC and OC [72], and the strong light-absorbing properties of BC partly explain the increased AAOD BC during winter. Figure 5a,b shows the variations of the annual ratios of AAOD BC to AOD T and AAOD BC to AOD nd at 440 nm and their trends for 2001-2018, respectively. The AAOD BC in Japan and Korea fell more greatly or more quickly than in Beijing, despite AOD T remaining stable at those sites. We attributed the difference in the ratios of AAOD BC /AOD T and AAOD BC /AOD nd between Beijing and the Korean and Japanese sites to Beijing's lower and/or slower reduction in BC emissions during the study period. Figure 5b shows that Beijing's ratio of AAOD BC /AOD nd declined at a rate of 0.0008 yr −1 , the lowest among the six sites. Hence, it can be concluded that Beijing's decrease in BC emissions relative to the other pollution particles was lower than that at the Korean and Japanese sites. This might be attributable to the delayed implementation of pollution control or fuel substitution policies, or a shift of, or even increase in, residential coal use and emissions from vehicles burning liquid fuel in Beijing compared to the Korean and Japanese sites. In other words, although BC emission control policies in China seem to have been successful during the past 18 years, BC still needs to be further reduced.
The ratio of AAOD BC /AOD nd showed an almost identical annual variation to the ratio of AAOD BC /AOD T in the Korean and Japanese sites. Polluted urban regions, such as Osaka, showed higher AAOD BC /AOD nd ratios during the study period than background cities, such as Anmyeon and Gosan, owing to higher BC concentrations. Another distinctive feature of Figure 5 is that Beijing generally had the highest values for both annual ratios from 2001 to 2018 (except for 2003). Beijing's severe urban haze that contains notable amounts of BC may account for its high AAOD BC /AOD T ratio. China has been reported to emit nearly a quarter of global anthropogenic BC due to its high usage of coal, oil, and biofuel [73,74]. Figure 6 represents that the seasonal variation of the annual AAOD BC /AOD T ratio (BC ratio) at 440 nm was higher during winter, and lower in summer at all sites. The common trend in BC ratio across the sites suggests similar reductions in BC emissions associated with the implementation of emission control measures over East Asia. A seasonal trend with summer minima and winter maxima was superimposed on this downward trend at all sites (except for Anmyeon). Regardless of the seasonal variation, Beijing showed the highest BC ratios as it had the highest BC emissions among the selected sites. Due to a lack of long-term regional-scale observational data, no consistent trend was identifiable for the Korean sites specifically in winter, but Gwangju had higher BC ratios than the other Korean sites (Anmyeon and Gosan) during all seasons. This is connected to Gwangju being a metropolitan city and a regional industrial center, with much coal-burning and other anthropogenic emissions that negatively affect air quality. Among the Japanese sites, Osaka had a higher BC ratio than Shirahama. Osaka is Japan's second largest urban area and has contributed greatly to Japan's economy and rapid industrialization over recent decades, which may explain its high BC ratio. Note that in addition to local emissions, the Korean and Japanese sites might be affected by aerosol loads transported from China by strong westerly winds [75].
According to Figure 7b, the monthly variation of BC ratio represents the highest values in Beijing, peaking in November, December, and January, and the lower values in August from 2001 to 2018. Summers in Beijing are rainy, and account for about 70% of the city's rainfall. The frequent rain probably lowered the concentration of BC, and consequently its AAOD, over Beijing in summer. The BC sources from October to March in Beijing are unlikely to be forest fires because of the cold weather. The increased BC ratio in this period was instead attributed to changes in major emission sources, specifically residential emissions. Qin et al. [67] suggested that transportation is the dominant emission source of BC in Beijing, with similarly high emissions in all seasons, while residential BC emissions greatly increase in winter. The Korean and Japanese sites showed lower BC ratios (below 0.10) than Beijing. The limited observation data for the Korean and Japanese sites may have resulted in them showing lower BC ratios. The highest values were in cold seasons (October to March), and the lowest values were during warmer seasons (June to September). Figure 7c shows that the monthly mean variations of the ratio of AAOD BC to AOD nd increased sharply from October to February, and was lowest in late summer (August) for Beijing. This suggests a higher contribution of BC to AAOD during the colder months (November to January) than at other times of the year. The average ratio of AAOD BC to AOD nd at 440 nm during 2001-2018 varied between 0.10 and 0.02 at the Korean and Japanese sites, with the Japanese sites showing higher values than those in Korea. Values were highest in December and January, and lowest in July and August. The residential sector was likely the main reason the ratio of AAOD BC to AOD nd increased during the colder months over these regions.
It is worth noting that in this study some errors arise from SSA D and SSA BC . As was mentioned in the materials and methods section, the value of 0.94 was used for SSA of East Asian dust at 440 nm [31], while in some other studies the value of 0.92 was applied for SSA D over Korea sites [48]. Besides, the value of 0.25 was applied for SSA BC at 440 nm; however, in some other studies, this value was reported to be 0.25 ± 0.13 [14]. In this study, the value of 0.25 ± 0.13 for SSA BC can cause negligible changes in AAOD BC values.

Conclusions
The long-term results for AOD T show that Beijing had the highest values, but its values are decreasing. The lower values in Korea and Japan showed no significant trend. This suggests that