A total of 85 total suspended particulate (TSP) samples were collected on the roof (57 m above ground level) of the Faculty of Environment at Kasetsart University (100∘57′ E and 13∘85′ N) in Bangkok, Thailand (Fig. S1 in the Supplement). Detailed information about the sampling site is presented elsewhere (J. Wang et al., 2020). Sampling was performed from 18 January 2016 to 28 January 2017, and the sampling period was divided into four seasons: the pre-hot season (18 January–28 February 2016), hot season (2 March–30 May 2016), monsoon (2 June–30 October 2016), and cool season (1 November 2016–28 January 2017). Table S1 lists the average meteorological data in the four seasons. Generally, during the sampling period, the hot season was characterized by high temperatures and wind speeds, and the monsoon season was characterized by high humidity. TSP samples were collected over 24 h using a high-volume (0.3 m3 min-1) sampler with quartz-fiber filters (QFFs, prebaked for 6 h at 450 ∘C). All samples and field blanks were stored under dark conditions at -20 ∘C until analysis.

WSOC was prepared by ultrasonication extraction of filter punches with ultrapure deionized water (resistivity of > 18.2 MΩ). The methanol-soluble OC (MSOC) fraction was then obtained by extracting the freeze-dried residue on the same QFFs after water extraction with HPLC-grade methanol, which is used for water-insoluble fractions (Chen and Bond, 2010). It is worth noting that the MSOC in this study is not necessarily like that of the same name in other studies. The extract solutions were passed through 0.22 µm PTFE filters and subjected to follow-up UV–Vis absorption and fluorescence spectral analysis. The mass concentrations of WSOC and MSOC were measured, and the methods are shown in the Supplement.

The extract solutions were placed in quartz cells with a path-length of 1 cm and subjected to analysis using a fluorometer (Aqualog; Horiba Scientific, USA). Absorption spectra and EEM spectra were obtained simultaneously using this instrument. The contribution of solvents was subtracted from the extract spectra. UV–Vis absorption spectra were scanned in the range of 239 to 800 nm with a step size of 3 nm. The fluorescence spectra were recorded with an emission wavelength (Em) ranging from 247.01 to 825.03 nm and excitation wavelength (Ex) ranging from 239 to 800 nm. The wavelength increments of the scans for Em and Ex were 4.66 and 3 nm, respectively. The calculation of optical parameters and the relative contributions of BrC to total aerosol light absorption are presented in the Supplement.

In this study, we built a PARAFAC model based on 85 TSP sample fluorescence (samples × Ex × Em: 85 × 188 × 125, 85-model). Original EEM spectra were corrected and decomposed via PARAFAC analysis with reference to earlier methods using drEEM toolbox version 2.0 with MATLAB software (http://models.life.ku.dk/drEEM, last access: June 2014) (Murphy et al., 2013; Andersson and Bro, 2000). The absorbance, all below 1 at 239 nm, was deemed suitable for correcting the EEM spectra for inner filter effects (IFEs) (Luciani et al., 2009; Gu and Kenny, 2009; Fu et al., 2015), and the sample EEM spectra and blanks were normalized relative to the Raman peak area of ultrapure deionized water collected on the same day to correct fluorescence in Raman units (RU) (Murphy et al., 2013, 2010). Spectra with Em > 580 nm and Ex < 250 nm were removed to eliminate noisy data. The non-negativity constraint is necessary to obtain reasonable spectra, and signals of first-order Rayleigh and Raman scattering as well as second-order Rayleigh scattering in the EEM spectra were removed using the interpolation method (Bahram et al., 2006). The two- to nine-component PARAFAC model was explored within the context of spectral loading, core consistency, and residual analysis (Figs. S2–S5). Finally, seven and six components were identified in the WSOC and MSOC fractions, which explained 99.89 % and 99.76 % of the variance, respectively. Both the seven- and six-component PARAFAC solutions passed the split-half analysis with the split style of S4C6T3, and residuals were examined to ensure that there was no systematic variation. The parameters obtained from the PARAFAC model were used to calculate the approximate abundance of each component, expressed as Fmax⁡ (in RU), corresponding to the maximum fluorescence intensity for a particular sample.

Fluorescence indices based on intensity ratios provide insight into the origins of dissolved BrC, such as the humification index (HIX) (the ratio of average emission intensity in the 435–480 nm range to that in the 300–345 nm range following excitation at 254 nm, which was used to reflect the degree of humification) (Zsolnay et al., 1999), the biological index (BIX) (the ratio of emission intensities at 380 and 430 nm following excitation at 310 nm, reflecting autochthonous biological activity in water samples) (Huguet et al., 2009), and the fluorescence index (FI) (the ratio of emission intensities at 470 and 520 nm following excitation at 370 nm, reflecting the possibility of microbial origin and for examining differences in precursor organic materials) (Lee et al., 2013; Murphy et al., 2018).

A hierarchical cluster method was used to classify aerosol samples based on the relative contributions of PARAFAC components to the respective samples. The squared Euclidean distance method was used to evaluate the distances between samples, and the between-group linkage method was chosen for hierarchical cluster analysis. The multiple linear regression (MLR) model was applied to elucidate the relationship between fluorescent chromophores and light absorption of BrC using a stepwise screening process. Analyses were performed using SPSS software (SPSS Inc., Chicago, IL, USA).

Fluorescence spectra coupled with PARAFAC results can provide more information about the chemical structures of chromophores. Figure 1 and Table S2 show the seven-component (P1–P7) PARAFAC solutions of WSOC in the samples of aerosol over Bangkok, the peaks of which fell mainly into the humic-like and protein-like chromophore regions in the plots. Components P2, P3, P4, and P6 were identified as humic-like substances (HULIS) (H. Chen et al., 2017; Stedmon and Markager, 2005; Wu et al., 2019; Chen et al., 2003). A second peak was observed at a high excitation wavelength for these components, indicating the existence of a large number of condensed aromatic moieties, conjugated bonds, and nonlinear ring systems (Matos et al., 2015). Among them, P2, P3, and P4 had a longer emission wavelength (> 400 nm) than P6, likely due to the low probability of fluorescence emission from quinonoid n-π∗ transitions (Cory and McKnight, 2005). P3 produced spectra similar to those of aqueous reaction products of hydroxyacetone with glycine (Gao and Zhang, 2018) and dissolved organic matter (DOM) in the surface water of Xiangxi Bay and Three Gorges Reservoir (Wang et al., 2019). P6 had a peak similar to those in the fluorescence spectra of N-containing SOA species formed by α-pinene under ozonolysis and photooxidation with NH3 in a flow reactor (Babar et al., 2017) as well as pyridoxine (Pöhlker et al., 2012), indicating a possible biological source. P5 was similar to a previously identified fluorophore in PM2.5 from Xi'an (Chen et al., 2019b). P1 and P7 could be assigned as protein-like organic matter (PLOM) due to their short emission wavelengths (Wu et al., 2003). Specifically, P7 resembled a tyrosine-like fluorophore (Zhou et al., 2019; Chen et al., 2003) and may be related to non-N-containing species (Chen et al., 2016b).

The MSOC fraction extracted from the filter residue after water extraction produced fluorescence signals with fluorescence patterns different from those of the WSOC fraction, indicating a different chemical composition from that of WSOC. Thus, WSOC with the addition of MSOC may provide a more comprehensive description of the optical and chemical characteristics of BrC compared to WSOC alone. Six components (C1–C6) were resolved for the MSOC. Among them, C1 and C2 were associated with shorter excitation wavelengths (< 250 nm) but longer emission wavelengths (> 380 nm), indicating the presence of fulvic-like substances (Chen et al., 2003; Mounier et al., 1999). C6 produced a pattern similar to that of tyrosine-like fluorescence (Stedmon and Markager, 2005). Although C4 had a similar EEM spectrum as P4 of WSOC, the two components were chemically different in polarity, suggesting different behaviors in the environment (Ishii and Boyer, 2012). Note that there were no special chemical structures for the different types of chromophores, and therefore the origins and chemical structures of HULIS and PLOM studied here are not necessarily like those with the same names in other types of organic matter.

To further explore the potential sources of the EEM–PARAFAC components, we added 60 source samples to the matrices. The source sample EEM data were described in our previous study (Tang et al., 2020b), including those of 33 biomass burning samples (IDs: 1–33), 17 coal-combustion samples (IDs: 34–50) samples, eight tunnel samples (IDs: 51–58), and two vehicle exhaust samples from trucks (IDs: 59–60), which are important sources of BrC in the atmosphere. This, in combination with our Bangkok field samples, yielded a new matrix (145 × 188 × 125, 145-model) for modeling. PARAFAC analysis successfully decomposed the dataset, and the output was the same as for the 85-model. The component solutions are presented in Fig. S6. To validate the stability of the model after loading by the new matrix, the Tucker congruence coefficient (TCC) was calculated to determine the similarity of two fluorescence spectra between the two models (refer to Text S3 of the Supplement). Note that a higher TCC value would indicate a higher degree of similarity of the spectra. As shown in Table S2 and Fig. S7, high TCC values were found as expected between the 85-model components and the 145-model components, indicating that the two models identified similar fluorescent chromophores. It should be noted that one additional fluorescent component each was identified for the WSOC and MSOC fractions in the new 145-model, but these components were only highly characterized by source emission samples, as reported in our previous study (Tang et al., 2020b).

Using the distribution proportions of the EEM–PARAFAC fitted components (145-model), we conducted hierarchical cluster analysis of the mixed ambient and source samples. The results are shown in Figs. S9 and S10. For the WSOC fraction, all aerosol samples from Bangkok and tunnel samples were assigned to cluster A, whereas biomass burning and coal-combustion aerosols were assigned to clusters C and D, respectively. This implied that the fluorescent chromophore types could be somewhat related to the emission precursors of the aerosol components. However, the distribution of fluorescent chromophores clearly varied between the ambient aerosols and source samples. The ambient aerosol samples contained higher levels of fluorescent chromophores with longer emission wavelengths that were related to humic-like or fulvic-like chromophores (components 145M-P1 – the P1 component in the 145-model, 145M-P5, and 145M-P6), whereas the primary biomass burning and coal-combustion samples contained high-intensity fluorescent chromophores with shorter emission wavelengths that were related to protein-like fluorescence (145M-P2 and 145M-P4). These phenomena was similarly reported previously; i.e., protein-like substances produce compounds with similar fluorescence properties as humic substances under irradiation conditions (Bianco et al., 2014). Similar differences between field samples and source samples were found for the MSOC fraction. Therefore, our results confirmed that chemical reaction or “aging” in the atmosphere greatly modifies the chromophore patterns of emission sources by both bleaching the source chromophores and producing new chromophores, and, at least in this case, it shifts the chromophore emission wavelength toward longer wavelengths, i.e., from protein-like to fulvic-like (Bianco et al., 2014, 2016; Lee et al., 2013).

The ratios of fluorescence intensity from specific spectral regions of an EEM were used as indicators for the relative contributions of organic matter derived from terrestrial or microbial sources in natural waters (Shimabuku et al., 2017; Birdwell and Engel, 2010; Mcknight et al., 2001). HIX was initially introduced to estimate the degree of maturation of DOM in soil (Zsolnay et al., 1999), representing the degree of humification of organic matter, for which higher HIX values also indicate a higher degree of polycondensation (low H / C ratio) and aromaticity (Qin et al., 2018). Generally, high HIX values (> 10) correspond to strongly humified or aromatic organics, principally of terrestrial origin, whereas low values (< 4) are indicative of autochthonous or microbial origin. As shown in Table 1 and Fig. 2, the HIX values were 3.4 ± 0.99 and 2.0 ± 0.59 for WSOC and MSOC, respectively, in aerosol samples from Bangkok. All HIX values were less than 10, which could be viewed as a nominal cutoff below which DOM is not significantly humified (Birdwell and Valsaraj, 2010; Zsolnay et al., 1999; Huguet et al., 2009). Figure 2 shows the HIX values in primary biomass burning and coal-combustion samples, which were much lower than those in the ambient samples, indicating that the lower values of HIX in the atmosphere likely correspond to freshly introduced material. Lee et al. (2013) reported that fresh SOA had low HIX values, but these values increased significantly upon aging with ammonia. The much higher HIX values in the WSOC compared to the MSOC suggest that WSOC may have a higher degree of aromaticity or a more condensed chemical structure. Our previous study revealed that MSOC has a higher molecular weight but lower aromaticity index than the corresponding WSOC in combustion experiment aerosol samples, indicating a more aliphatic structure in the MSOC (Tang et al., 2020b). The HIX values of WSOC were highest in the hot season (3.9 ± 1.1), followed by the pre-hot season (3.3 ± 1.1), cool season (2.9 ± 0.36), and monsoon (2.5 ± 0.22), whereas those of the MSOC tended to be higher in the hot and cool seasons than in the monsoon and pre-hot seasons. The HIX values in the WSOC fraction were comparable to those of water-soluble organic aerosols in the high Arctic atmosphere (mean: 2.9) (Fu et al., 2015) and higher than those of water-soluble aerosols (1.2 ± 0.1 in winter and 2.0 ± 0.3 in summer) over northwestern China (Qin et al., 2018), likely indicating a higher degree of chromophore humification.

The BIX and FI were previously proposed as proxies for the contribution of biogenic organic matter and autochthonous biological activity in natural water, respectively (Fu et al., 2015; Qin et al., 2018). For example, the FI decreased by up to 20 %, indicating that the samples appeared increasingly like “terrestrial” DOM, whereas the BIX increased by up to 37 %, indicating that the samples became more “autochthonous” in character (Murphy et al., 2018; Gabor et al., 2014). FI values ≤ 1.4 correspond to terrestrially derived organics and higher aromaticity, whereas values ≥ 1.9 correspond to microbial sources and a lower aromatic carbon content (Mcknight et al., 2001). An increase in BIX is related to an increase in the contribution of microbially derived organics, with high values (> 1) shown to correspond to a predominantly biological or microbial origin of DOM and the presence of organic matter freshly released into water, whereas values ≤ 0.6 indicate the presence of little biological material (Huguet et al., 2009).

The FI and BIX values of the Bangkok aerosol samples are summarized in Table 1 and Fig. 2. The FI values of the WSOC and MSOC were 1.6 ± 0.10 and 1.8 ± 0.20, respectively, suggesting that these chromophores are representative of both terrestrially and microbially derived organic matter. The BIX values of the WSOC and MSOC were 0.82 ± 0.13 and 1.2 ± 0.18, respectively. Almost all BIX values were greater than 0.6 in the two fractions, suggesting biological or microbial contribution. Lee et al. (2013) reported that the BIX values of SOA samples averaged 0.6 and increased upon aging. In addition, the results of our source samples showed that primary biomass burning and coal-combustion samples had high FI and BIX values (Fig. 2). These results indicate that these chromophores in Bangkok were likely freshly introduced or derived from biomass burning and coal combustion. Further, an increase in BIX in the MSOC in comparison with the WSOC was observed in primary biomass burning and coal-combustion samples, consistent with the Bangkok samples. The BIX values were similar to those in the WSOC in Arctic aerosols (0.6–0.96, mean: 0.72), which were within the extreme values for the predominance of humic- or protein-like fluorophores (Fu et al., 2015). BIX values exhibited the opposite trend from HIX values, with low BIX values in the hot season. This may be explained by a previous study showing that a high BIX appears to indicate little humification (Birdwell and Engel, 2010). It should be noted that the fluorescence indices (FI, BIX, and HIX) were first applied for aquatic and soil organic compounds and further extended to the atmosphere due to the similarities in the properties of organic matter (Graber and Rudich, 2006). However, the values observed for primary biomass burning and coal combustion in this study differ from the previously established fluorescence standards for aquatic environments and soil. Therefore, caution is required when using these indices to appoint the source of atmospheric chromophores (Wu et al., 2021).

Figure 3 shows the variations in soluble OC concentrations and the corresponding light absorption coefficient at 365 nm (Abs365). In general, the Abs365 closely tracked the variations in the mass concentrations of WSOC and MSOC (p < 0.000, R2=0.95 and p < 0.000, R2=0.75, respectively) (Fig. S11), indicating that the portions of BrC in both fractions were considerably stable. Furthermore, light absorption at 365 nm was higher in the pre-hot season, hot season, and cool season than that in the monsoon season. According to the levoglucosan level, which is generally regarded as a biomass burning tracer, and the ratios of levoglucosan / TSP (Table 1), we infer that the non-monsoon season was more affected by biomass burning and also showed high absorption.

The absorption Ångström exponent (AAE) and mass absorption efficiency (MAE) are important optical parameters reflecting the spectral dependence and light absorption ability of BrC, respectively. The magnitude of the AAE reflects the differences in BrC source and atmospheric processes (Lack et al., 2013). Typically, the AAE value is close to 1 when light absorption is dominated by soot (Kirchstetter et al., 2004), roughly 1–3 for simulated biomass burning aerosols (Hopkins et al., 2007), and up to 6–7 for water-soluble HULIS in biomass-burning-impacted aerosols (Hoffer et al., 2006). The AAE values of the WSOC and MSOC between 330 and 400 nm in this study were up to 5.1 ± 0.68 and 5.2 ± 0.94 (Fig. 4), respectively, indicating strong wavelength dependence in the light absorption capability. These high values show that BrC tends to absorb more solar irradiation over ultraviolet wavelengths, which is comparable to BC absorption as shown in Fig. S12. These observations indicate that BrC has important impacts on photochemical reactions in the atmosphere (Barnard et al., 2008). The AAE values in this study are similar to those of water-soluble BrC over biomass-burning-impacted regions, such as Beijing (Mo et al., 2018; Yan et al., 2015) and Guangzhou (Liu et al., 2018), but lower than those of aerosols from simulated biomass burning and coal-combustion experiments (Fan et al., 2018; Tang et al., 2020a; Li et al., 2018). However, it should be noted that the BrC AAE varies in the atmosphere. Dasari et al. (2019) reported that AAE values of water-soluble BrC increase continuously due to photolysis of chromophores and atmospheric oxidation during long-range transport over the Indo-Gangetic Plain (IGP). In addition, pH changes can cause the absorption spectra of some BrC species to shift to longer wavelengths upon deprotonation, decreasing AAE values (Mo et al., 2017). The pH values of the WSOC fraction for all the samples were within the range of 5–7, generally indicating no effect on the absorbance according to a prior study (Chen et al., 2016a).

The MAE at 365 nm (MAE365) of the WSOC was 0.83 ± 0.25 m2 g-1 C, which was higher than that of the MSOC (0.26 ± 0.12 m2 g-1 C), indicating that more water-soluble BrC with stronger light absorption capability could be extracted with ultrapure deionized water, whereas water-insoluble BrC is characterized by lower light absorption capability over Bangkok. These results are consistent with those from vehicular exhaust samples in our previous study, wherein MAE365 values of the WSOC (0.71 ± 0.30 m2 g-1 C) were higher than those of the MSOC (0.26 ± 0.09 m2 g-1 C) (Tang et al., 2020b). Opposite results have been shown for primary biomass burning and coal combustion (Tang et al., 2020b). Similarly, Bikkina et al. (2020) observed that the marine-impacted aerosols of the Bay of Bengal showed higher MAE365 values in the WSOC fraction than the MSOC fraction (only extract using methanol), and they explained it due to two plausible reasons. First, the BrC aerosols over the Bay of Bengal have a contribution from a different source (i.e., maritime influence) and contain BrC chromophores that are more soluble in water than methanol. Second, there could be significant photobleaching effects of different chromophores. However, G. Wu et al. (2020) reported that the MAE365 values of methanol extracts are higher than those of WSOC in summer, whereas the situation is reversed in winter. Therefore, we infer that the different sources and atmospheric processes would impact the distribution of water-soluble and methanol-soluble chromophores. The high temperature and humidity (Table S1) and the tropical monsoon climate in Thailand seem to promote more water-soluble chromophores over Thailand. As not all water-insoluble components can be extracted with methanol, the observed light absorption by MSOC would therefore likely reflect the lower limit. Table S3 shows a comparison of the MAE values of Bangkok aerosols with those of other regions, indicating a medium light absorption capacity. The MAE365 values of the water-soluble fraction in this study were comparable to those of Nanjing (Chen et al., 2018), Guangzhou (Liu et al., 2018), and Beijing in summer (Yan et al., 2015) but lower than those of PM2.5 from Singapore (Adam et al., 2020), PM10 from Godavari, Nepal, in the pre-monsoon season (Wu et al., 2019), and smoke particles from biomass burning and coal combustion (Park and Yu, 2016; Fan et al., 2018; Tang et al., 2020b). Lower MAE365 values of both fractions were observed in the monsoon season than in the non-monsoon seasons, likely due to the heavy monsoon rains that effectively remove soluble gases and aerosols (Lawrence and Lelieveld, 2010) and/or reduce biomass burning activity (levoglucosan level in Table 1). A previous study reported similar findings in the USA in that the MAE365 was approximately 3-fold higher in biomass-burning-impacted samples than in non-biomass-burning-impacted samples (Hecobian et al., 2010). Another study in the central Tibetan Plateau highlighted the fact that BrC emitted by biomass burning has stronger light absorption capability than secondary BrC formed in the atmosphere (Wu et al., 2018). On the Indo-China peninsula, Bangkok receives 99 % of the fire-derived aerosols from December to April (Lee et al., 2017), which may explain the high absorption levels in the non-monsoon seasons.

EEM analysis enables the probing of the chemical structure of DOM because of its ability to distinguish among different classes of organic matter (Wu et al., 2003). Generally, BrC absorption is related to the chromophores within it and is susceptible to change with variations in chemical properties, e.g., oxidation level (Mo et al., 2018), degree of unsaturation (Jiang et al., 2020), molecular weight (Tang et al., 2020b; Di Lorenzo et al., 2017), functional groups (Q. Chen et al., 2017), and molecular composition (Song et al., 2019; Lin et al., 2018). The fluorescence intensity of each EEM component was shown to be associated with light absorption indices, such as MAE365 and AAE, of HULIS in controlled crop-straw-combustion experiments (Huo et al., 2018). As a linear relationship between organic matter concentration and fluorescence intensity can be assumed for very dilute samples due to the IFE (Murphy et al., 2013), we have corrected our fluorescence data for IFE using absorbance to enable “clean” correlation analysis (as shown in Fig. S13a, b). The linear regression slopes in the scatter plots of Abs365 versus WSOC or MSOC could mathematically represent the average MAE values of WSOC or MSOC at 365 nm, respectively (Fig. S11a, b). The phenomenon indicates that both fluorescence and Abs365 data point to similar relationships between sources or chemical processes with organic matter concentrations, and therefore we attempted to link the fluorescence results to BrC absorption. It should be noted that light-absorbing substances in atmospheric particulate matter are not necessarily all fluorescent, such as nitrophenol compounds, which are a type of BrC commonly found in the atmospheric particulate matter; however, there is no strong fluorescence signal with which to scan the nitrophenol standards (Chen et al., 2019a).

In order to evaluate the light absorption from different fluorescent chromophores, we used MLR to explore the relationship between the fluorescence intensities of chromophores and Abs365. In this study, light absorption properties were treated as the dependent variables, and the fluorescence was an independent variable. During MLR, insignificant fluorescent components were excluded from the regression using a stepwise screening process to avoid overfitting (Finclusion: p < 0.05; Felimination: p > 0.10). The MLR statistical metrics are listed in Tables S4 and S5. For the independent variables with significant correlations with the dependent variable (p < 0.05) or with positive contributions to the independence, Abs365, they will be retained in the statistical model as the efficiency factors to Abs365. Thus, for the WSOC fraction, a revised model (regression 3) equation was used with an adjusted R2 of 0.995. The final optimized equations were Abs365 = 0.765 × P4 + 0.051 × P2 + 0.091 × P7 for the WSOC fraction and Abs365 = 0.238 × C4 for the MSOC fraction (Table S5). The model errors for water-soluble and methanol-soluble Abs365 were -5.5 %–64 % and -34 %–58 %, respectively. The predicted Abs365 values fit the measured values well (Fig. 5; slope = 0.99 and 0.95, R2 = 0.99 and 0.94 for WSOC and MSOC, respectively).

For water-soluble BrC, the P4 component had the largest coefficient with Abs365, which was much higher than those for P2 and P7. The C4 component had the largest coefficient with Abs365 for methanol-soluble BrC. These results indicate that the light absorption by BrC is more dependent on chromophores with longer emission wavelengths (P4 and C4). These characteristics also indicate that the strongly absorbing substances in BrC probably originate from large conjugated electron functional groups or include donor and acceptor molecules for charge–transfer interactions (Del Vecchio and Blough, 2004; Cory and McKnight, 2005). Kellerman et al. (2015) reported that these components are highly aromatic and oxygen-rich with a high apparent molecular weight. These important findings highlight the fact that larger chromophores may be the most persistent BrC species in the atmosphere and hence exert the greatest influence for perturbing the global radiative balance.

To further interpret the BrC source profiles as real-world TSP sources, we examined 84 (minus one missing value) TSP samples from Bangkok using the US EPA PMF5.0 model. All samples were merged together to form an 84 × 30 dataset (84 samples with 30 species). The initial data of positive matrix factorization input were from our previous study (J. Wang et al., 2020). We further added Abs365 values of WSOC and MSOC, as well as the fluorescence intensities (in RU) of P2, P4, P7, and C4 components to the model. A seven-factor solution was achieved that provided the most physically reasonable source profiles (Fig. S14), including ship emissions, secondary sulfate, dust, land fossil-fuel combustion, sea salt, biomass burning, and industrial emissions, consistent with our previous study (J. Wang et al., 2020). Figure S15 shows the contributions of the above sources to light absorption at λ = 365 nm, which represent the fraction of BrC for each factor. Biomass burning was found to be the main source of BrC over Bangkok: 58 % and 74 % for water-soluble and methanol-soluble BrC, respectively. These were comparable to previous observations using a similar approach in Xi'an (55 %) (C. Wu et al., 2020). The time series of Abs365 of WSOC and MSOC contributed by factors shows that the high biomass burning contribution is related to the higher local fire spots (i.e., pre-hot season, hot season, and cool season) and/or air mass from the continent (Figs. S16–S17). Jiang et al. (2021) observed increases in biomass burning contributions to BrC absorption during the winter period that was dominant in continental-origin air masses. Furthermore, the P4 and C4 components, which were more closely associated with Abs365, could be mostly attributed to biomass burning (54 % and 70 %, respectively) as shown in Fig. 6. Our previous study showed that biomass burning accounted for a considerably large portion (mean: 26 %) of the TSP mass concentration in the same samples (J. Wang et al., 2020). This result suggests that biomass burning makes a significant contribution to not only particulate matter but also BrC light absorption.