Shipboard cruise observations were conducted over the Bohai Sea and the Yellow Sea (YBS) during autumn (22 October–2 November) in 2021 and during spring (13–28 April) and summer (13 July–13 August) in 2023. During the campaigns, total suspended particles (TSP) and fine particles (PM_2.5) were simultaneously collected on prebaked quartz fiber filters using a high-volume aerosol sampler (1.05 m³ min⁻¹). The sampler was placed at the front of the upper deck to avoid potential contamination from ship exhaust. Each sample was collected for 15–20 h, ensuring sufficient mass loading for the following chemical analysis. A total of 9, 22, and 20 sets of aerosol samples were obtained during the autumn, spring, and summer cruises, respectively. Due to difficult marine conditions and the tight schedule of the vessel in autumn, 9 sets of aerosol samples were collected during the autumn cruise. Aerosol samples were collected continuously along the cruise when the ship was sailing, and sampling covered the whole observation region of the YBS. Thus, the samples can represent the general conditions of the YBS in each season. A field blank sample was collected during each cruise.

Air temperature and relative humidity (RH) were monitored using an onboard meteorological station during the observations. The 72 h backward trajectories of air masses at an altitude of 500 m were calculated using the HYSPLIT model (Fig. S1 in the Supplement) (Zhang et al., 2025), which can represent the marine boundary layer (Huang et al., 2018). Satellite-derived chlorophyll a (Chl a) in surface seawater was obtained from NASA Ocean Color (https://oceancolor.gsfc.nasa.gov/, last access: 21 April 2026).

Total ON in aerosol samples was determined using an aerosol IN&ON analyzer system, which integrates an online aerosol carbon analyzer and a NO_x analyzer (Yu et al., 2023b). Programmed thermal evolution facilitates the separation of aerosol ON from IN, and quantification of ON is achieved through multivariate curve resolution treatment of carbon and nitrogen thermal fractions (Yu et al., 2021). The IN&ON analyzer has been widely used to quantify aerosol ON from various atmospheric environments. Water-soluble organic carbon (WSOC) and water-soluble total nitrogen (WSTN) are analyzed by the TOC/TN analyzer (TOC-L, Shimadzu, Japan). Inorganic nitrogen (NO3-–N and NH4+–N), other inorganic ions (SO42-, Cl⁻, Na⁺, K⁺, Ca²⁺, Mg²⁺), methanesulfonic acid (MSA), and oxalic acid were quantified using ion chromatograph systems (ICS‐Aquion, ICS‐2100 DIONEX). Concentrations of WSON and WION were calculated as follows: 1WSON=WSTN-[NH4+–N]-[NO3-–N]2WION=ON-WSON The abundance of inorganic nitrogen quantified by the aerosol IN&ON analyzer or by the TOC/TN analyzer matched well with that measured by ion chromatograph (Fig. S2), which guarantees the accuracy of quantitative results of WSON and WION based on different analytical methods. The detection limit of aerosol IN&ON analyzer was 96 ng N, and that of TOC/TN analyzer was 0.01 µg N mL⁻¹. Based on the measurement results of aerosol IN&ON analyzer, total nitrogen in the field blank samples was 0.040–0.068 µg N cm⁻², much lower than that in the collected aerosol samples (0.49–44.2 µg N cm⁻²). Total nitrogen on the corresponding field blank sample was subtracted from each sample.

Organic carbon (OC) and elemental carbon (EC) in atmospheric aerosols were measured using a carbon analyzer (Sunset Laboratory) based on thermal-optical method. Water-insoluble organic carbon (WIOC) was calculated by the difference between OC and WSOC. Concentration of organic matter (OM) in the aerosol samples was calculated by multiplying OC by 1.6 (Turpin and Huntzicker, 1995; Wang et al., 2023b). Our previous observations over the YBS suggested that organics were dominant in fine particles (Zhang et al., 2025). Thus, we mainly focused on the PM_2.5 results for further discussion, and concentrations of Ca²⁺ in TSP were only used to identify the dust episode.

Light absorption properties of extracted organic aerosols were measured using a UV-visible spectrometer (UV-8000, Jingmi, China). Methanol and water were used to extract total organic matter and water-soluble organic matter (WSOM) in aerosols. Absorption spectra of the extracted solutions were detected using a UV-visible spectrometer within the wavelength range of 200–700 nm. Absorption coefficients (Abs_λ, Mm⁻¹) and mass absorption efficiency (MAE_λ) at a wavelength λ were calculated using the following equations: 3Absλ=(Aλ-A700)×Vl×ln⁡(10)L×Va4MAEλ=AbsλC where Aλ is the measured absorbance of extracted solutions at wavelength λ. A700 is used to correct the baseline shift of the UV-visible spectrometer during analysis. The L is the optical path length (10 mm). Vl and Va are the volumes of the extraction solution and the air passing through the extracted filters. The light absorption of methanol-soluble components was used to represent the absorption by total organic aerosols. The difference between methanol-extracted solutions and WSOM was the absorption by water-insoluble organic matter (WIOM).

To identify the aerosol ON from different sources, we used the positive matrix factorization (PMF) receptor model (PMF version 5.0, EPA) to apportion the sources of aerosol ON, WION, and WSON over the YBS. Measured concentrations of components in the PM_2.5 samples were used as the input parameters of PMF, including OC, EC, WSOC, MSA, oxalic acid, ON, WION, WSON, and Abs₃₀₀ by WIOM and WSOM, water-soluble cations (NH4+, K⁺, Na⁺, Ca²⁺, Mg²⁺), and water-soluble anions (SO42-, NO3-, Cl⁻). The Abs₃₀₀ of WIOM and WSOM were included as variables to be apportioned rather than tracers. Uncertainties (Unc) of the parameters were calculated according to the EPA PMF 5.0 user guide: 5Unc=EF×c)2+(0.5×MDL2 where EF is the error fraction, c is the concentration, and MDL is species-specific method detection limit. Data below MDL were replaced with the value MDL / 2, and (5/6) × MDL was used as the corresponding uncertainty value (Polissar et al., 1998). For the PMF analysis, a noticeably decreased Q/Qexp value suggests an improved solution, and the parameters experience less dramatic change (Wang et al., 2018). Figure S3 shows the variations of Q/Qexp with different solution numbers, and a five-factor solution is selected. Base Model Displacement and bootstrap combined displacement methods (BS-DISP) were used to assess the robustness of the PMF results. In the BS-DISP uncertainty estimation method, 85 % of the runs were acceptable and no factor swaps were observed. According to the EPA PMF user guide and previous studies (Brown et al., 2015; Paatero et al., 2014), > 80 % indicates that the uncertainties can be interpreted and the number of source factors may be appropriate.

Spatial variation and time series of ON in the collected PM_2.5 samples are shown in Fig. 1. The average concentration of ON in marine aerosols was 0.35 ± 0.25 µg N m⁻³ during the cruise observations over the YBS. The campaign-averaged concentrations of NO3-–N and NH4+–N were 0.63 ± 1.06 and 1.59 ± 2.14 µg N m⁻³, respectively. Organic nitrogen averagely accounted for 22 % (range: 4 %–60 %) of the total nitrogen (ON + NH4+–N + NO3-–N) and 6 % (range: 2 %–13 %) of organic matters in marine aerosols over the YBS. The observed aerosol ON over the YBS was among the ranges reported in previous studies over Mediterranean or Asian marginal seas (0.16–1.05 µg N m⁻³) (Sun et al., 2026; Tian et al., 2023; Violaki and Mihalopoulos, 2010), and lower than those in polluted continental environments (0.26–2.4 µg N m⁻³, e.g., urban Beijing, coastal Qingdao sites) (Shi et al., 2010; Wu et al., 2021; Xu et al., 2017). Under the joint influence of terrestrial transport and marine emissions, ON abundance in aerosols over the YBS was higher than that reported over open oceans (4.7–170 ng N m⁻³), such as the Southern Ocean, Atlantic, and Pacific Ocean (Luo et al., 2018; Matsumoto et al., 2022; Miyazaki et al., 2011; Sun et al., 2026; Violaki et al., 2015; Wang et al., 2026). Recent observations suggested that external aerosol organic nitrogen from transported combustion emissions or aged anthropogenic pollutants is important in the West Pacific Ocean (Ito et al., 2014; Wang et al., 2026). On a global scale, ON contributed 23 % of atmospheric total nitrogen deposition in marine ecosystems (Li et al., 2023).

Aerosol ON over the YBS exhibited clear seasonal variations (Fig. 2), following the abundance order of autumn (0.50 ± 0.32 µg N m⁻³) > spring (0.37 ± 0.24 µg N m⁻³) > summer (0.27 ± 0.18 µg N m⁻³). The relative standard deviation (RSD) of ON concentrations in marine aerosols was comparable across seasons (70 %, 65 %, and 69 % for the autumn, spring, and summer samples). The average ON concentrations in autumn and summer were significantly different at the 0.05 level, while differences between other seasons were not significant. The observation regions were dominated by continental air masses in autumn and spring and by marine air masses in summer (Fig. S1). Under the severe impacts of continental air mass outflows, aerosol ON in autumn or spring was higher than that in summer (Figs. 1, 2). Concentrations of K⁺ and NO3- in the collected samples were the highest during the autumn cruise (0.26 and 8.20 µg m⁻³) than during the other two seasons (0.066 and 1.37 µg m⁻³ in spring, 0.076 and 1.82 µg m⁻³ in summer), indicating the severer impacts of biomass burning and anthropogenic pollutants in autumn. In addition, a dust episode was observed during 12–16 April during the spring cruise (Fig. 1d), when Ca²⁺ concentrations in TSP increased obviously to 1.36–4.47 µg m⁻³, twice higher than the average values during the non-dust period (0.64 ± 0.30 µg m⁻³) in spring. During the dust episode, ON abundance increased to 0.57 ± 0.30 µg N m⁻³, higher than the ON concentrations observed on non-dust days during the spring cruise. The seasonal variation of aerosol ON was different from that of OC in marine aerosols, with an abundance order of spring (4.8 µg C m⁻³) > autumn (3.4 µg C m⁻³) > summer (2.7 µg C m⁻³). The dust storms in spring lead to a more obvious elevation of OC than ON in marine aerosols. It is noted that we only used the Ca²⁺ data in TSP to reflect the variation of coarse particles and identify the dust episode more clearly in this work. Other analyses were based on the PM_2.5 results, as previous observations have suggested that the organic mass and its absorption were dominant in fine particles over marginal seas (Zhang et al., 2025).

During the observations over the YBS, WSON (0.21 ± 0.15 µg N m⁻³) in marine aerosols was higher than WION (0.15 ± 0.12 µg N m⁻³). Previous studies suggested that aged or secondarily formed organic aerosols tend to be more soluble than primarily emitted organic aerosols (Fang et al., 2023; Zhang et al., 2025). For example, abundant WSON can be formed via oxidation of volatile organic compounds (VOCs) in the presence of anthropogenic NO_x or in NH₃-aged organic aerosols (Laskin et al., 2015). East Asian marginal seas are obviously influenced by continental air pollutants, which undergo oxidation and aging processes during transport, thereby contributing to water-soluble ON in marine aerosols over the YBS. Higher WSON / WION ratios indicated an elevated contribution of aged anthropogenic pollutants in marine aerosols over marginal seas. The water-insoluble fractions of aerosol ON were higher in spring (43 %) or summer (42 %) than in autumn (36 %). Our recent observation suggested that long-range transport of Asian dust is a major source of water-insoluble organic aerosols in spring over the East Asian marginal seas (Zhang et al., 2025). The proportion of water-insoluble ON among the total aerosol ON increased under the influence of spring dust storms. During summer, dominated by marine air masses, the relative contribution of marine-related sources increased. This resulted in a higher proportion of water-insoluble ON in summer than in autumn (Fig. 2). A previous study over the open Northwest Pacific Ocean reported an average WION / ON ratio of 55 %, and the contribution increased to 93 % at 40–44° N (Miyazaki et al., 2011), much higher than the fraction of WION over the YBS. Miyazaki et al. (2011) suggest that marine biological sources significantly contributed to WION in marine aerosols. Marine biological activities emit nitrogen-containing organic components (e.g., protein-like macromolecules), which can be emitted to marine aerosols and contribute to WION (Chen et al., 2016; Facchini et al., 2008).

Inter-species correlation and PMF source apportionment were analyzed to investigate the sources of aerosol ON over the YBS. As shown in Fig. S4, a five-factor solution was identified as a reasonable and stable result. The resolved source factors include: (1) aged biomass burning, characterized by high loadings of K⁺, EC, WSOC, and secondary inorganic ions; (2) dust-related formation, dominated by mineral dust tracers (Ca²⁺ and Mg²⁺); (3) secondary nitrate formation, with high loadings of inorganic nitrate aerosols; (4) Marine biogenic emission, characterized by MSA, a typical atmospheric oxidation product of dimethyl sulfide emitted by phytoplankton (Kurosaki et al., 2022; Stefels et al., 2007); (5) Sea spray aerosol, dominated by Na⁺, Cl⁻, and MSA. The PMF-resolved ON, WSON, and WION from different sources matched well with the measured concentrations in marine aerosols (Figs. S5, S6). Both aged biomass burning and secondary nitrate formation were anthropogenic secondary pollutants. The two factors are characterized by different tracers (Fig. S4) and showed different temporal variations (Fig. S7) during the observations, which thus were resolved as two separate sources.

Anthropogenic secondary pollutants, including aged biomass burning and secondary nitrate formation, were important sources of organic nitrogen in atmospheric aerosols over the YBS. The concentrations of ON, WSON, and WION showed moderate or strong correlations with K⁺ and nitrate in marine aerosols (Fig. 3). The source apportionment result suggested that aged biomass burning and secondary nitrate formation totally contributed 36 %–76 % of ON, 46 %–83 % of WSON, and 39 %–89 % of WION during the observations (Fig. 4). Driven by continental air masses, the concentrations of K⁺ and nitrate in the collected aerosol samples were much higher in autumn (0.26 ± 0.15 and 8.2 ± 9.1 µg m⁻³) than in the other two seasons (0.066 ± 0.050 and 1.4 ± 1.1 µg m⁻³ in spring, 0.076 ± 0.056 and 1.8 ± 2.1 µg m⁻³ in summer). The autumn samples were generally under severe impacts of transported anthropogenic pollutants, with 59 %–86 % of aerosol ON contributed by anthropogenic secondary formation. Aerosol ON contributed by anthropogenic sources substantially exceed that by dust-related or natural sources (marine biogenic emission and sea spray aerosol) during the autumn cruise (Fig. 4).

Previous studies have suggested that biomass burning and VOC oxidation with NO_x involved in would produce atmospheric ON in terrestrial environments (Liu et al., 2019; Wang et al., 2019b), which can be long-range transported to marine atmosphere. For example, methyl-nitrocatechols can originate from the oxidation of VOCs emitted by biomass burning (Iinuma et al., 2010). Nitro-aromatic compounds (e.g., nitro-phenols, nitro-catechol, and their derivatives) can be formed via oxidation of anthropogenic toluene and benzene under high-NO_x conditions (Wang et al., 2019b). Under mild aqueous-phase conditions, nitration of guaiacol can produce nitroguaiacols via the nonradical mechanism (Kroflic et al., 2018). Secondary formation of aerosol ON was typically associated with aqueous reaction processes (Chen et al., 2026). The contribution of aged biomass burning to WSON was higher than that to WION in aerosols (Fig. 4). Biomass burning is an important contributor to water-soluble organic components in the atmosphere, and aged organic aerosols tend to be more water-soluble than primarily emitted organic aerosols. A recent study suggested that wildfires contributed 37 % of global atmospheric ON deposition and that 40 %–80 % of total N deposition was attributable to aerosol ON downwind of biomass burning areas (Li et al., 2023).

We noted that ON abundance from secondary nitrate formation increased with the increase in RH in autumn (Fig. S8), with a correlation coefficient of 0.78 (p < 0.05). High-humidity conditions favor the secondary formation of aerosol ON via heterogeneous or aqueous-phase reactions. For example, high RH promotes the aqueous formation of nitrated aromatic compounds (e.g., methyl-nitrocatechols) (Shi et al., 2023; Vidovic et al., 2018; Wang et al., 2019b). Nitration of guaiacol can produce nitroguaiacols via the nonradical mechanism under aqueous-phase conditions (Kroflic et al., 2018). Aqueous reactions between dicarbonyls and ammonium, amine, or amino acids produce N-heterocycle compounds (De Haan et al., 2009; Marrero-Ortiz et al., 2019). For the spring samples, abundance of ON from secondary nitrate formation also showed an increasing trend with RH, but their correlation was not significant (p > 0.05). During the summertime cruise, however, we did not observe the influence of ambient RH on aerosol ON from secondary nitrate formation (Fig. S8c). The different dependence of ON formation on ambient RH was due to the higher RH in summer (79 % ± 7 %) than in spring (61 % ± 18 %) and autumn (54 % ± 9 %). Ambient humidity was not a limiting factor for aqueous formation of secondary organic aerosols (SOA) under the high RH in summer (Wang et al., 2023a). Under the low-RH conditions in autumn, humidity can be a more important limiting factor for ON formation, and elevated RH would favor its formation via aqueous reactions. Our results indicated that increased ambient RH promoted the formation of light-absorbing ON in marine aerosols. It is noted that we cannot distinguish the gas-phase and aqueous-phase formation pathways based on the PMF analysis here. The resolved ON from secondary nitrate formation included both the aqueous-phase formation pathway as well as the gas-phase formation and further gas-to-particle partitioning pathway.

During the spring cruise, ON, WSON, and WION showed strong positive correlations with Ca²⁺ in the aerosol samples (Fig. 3), indicating dust storms as an important source of aerosol ON over the YBS. However, the correlations between ON and Ca²⁺ during the other two seasons were weaker than in spring (Fig. 3). Based on the PMF result, contribution of dust-related formation to ON, WSON, and WION in marine aerosols elevated to 55 %, 45 %, and 54 % in spring, compared to 6 %–11 % in autumn and summer (Fig. 4). As shown in Fig. 1, a dust storm originating in Mongolia was recorded in spring (Wang et al., 2025; Zhang et al., 2025). The highest Ca²⁺ concentration was observed on 12 April. Based on the source apportionment result, 95 % of ON, 83 % of WSON, and 88 % of WION were attributed to dust-related formation on 12 April during the dust episode (Fig. S5). On one hand, dust surface favors the gas-to-particle partitioning or the uptake of gaseous organic precursors (Li et al., 2025c). On the other hand, aged dust particles could facilitate the formation of SOA via aqueous-phase or heterogeneous reactions, especially on nitrate-coating particles (Li et al., 2025a). For the spring samples, dust-related ON formation displayed a positive correlation with nitrate aerosol concentration (Fig. S9), indicating the secondary formation of ON on dust particles via mixing with nitrate aerosols. Mineral components provided favorable conditions for heterogeneous nitration reactions and further ON formation in aged dust particles coated by nitrate (Kroflic et al., 2018; Nie et al., 2014). Dust storms, mixing with anthropogenic nitrate pollutants during transport through East Asia, are a major contributor to inorganic and organic nitrogen deposition in marginal seas. Based on our previous study (Zhang et al., 2025), dust contributed 50 % of water-soluble OC and 70 % of the water-insoluble OC in marine aerosols during the spring cruise, higher than that to WSON (45 %) and WION (54 %) resolved in this work. The higher contribution of spring dust to aerosol OC than ON, especially for the water-insoluble fractions, explained their different seasonal variations. The aerosol ON formation, however, was more driven by anthropogenic secondary pollutants, and thus aerosol ON was higher in autumn than in spring. Dust-related aerosol ON likely formed during the long-range transport of dust storms via mixing with anthropogenic pollutants.

Marine sources, including marine biogenic emissions and sea spray aerosol, became a dominant contributor to ON in summer, accounting for 53 % of ON, 45 % of WSON, and 52 % of WION in aerosols over the YBS (Fig. 4). Marine-related ON was mainly associated with biogenic emissions. Amino acids, protein-like organic matter, urea, or other organic nitrogen compounds can be emitted from the ocean and enriched in marine aerosols (Matthews et al., 2023; Shi et al., 2010; Triesch et al., 2021; Wang et al., 2016). Marine-derived organic aerosols are usually enriched in fluorescent components related to marine biological activity (Miyazaki et al., 2018). These marine-generated reduced ON components are generally with lower light absorption capability compared with anthropogenic ON transported from the continent (Laskin et al., 2015). Marine biogenic emissions contributed 6 %–11 % of ON, 7 %–9 % of WSON, and 6 %–10 % of WION during the autumn and spring cruises, higher than the contribution of sea spray aerosols (< 3 %). Previous studies have suggested that marine-generated ON is usually related to biological activity or nitrogen-fixing microorganisms in seawater (Aller et al., 2017; Dobashi et al., 2023).

A recent study suggests that brown nitrogen, the absorptive nitrogenous components of organic aerosols, dominates their light absorption (Li et al., 2025b). Brown nitrogen contributes 76 % of surface light absorption by organic aerosols over the US and 61 % of their global absorptive optical depth (Li et al., 2025b). To understand the role of ON in regulating the absorption of marine organic aerosols over the East Asian marginal seas, we analyzed the correlations between aerosol ON and light absorption (Abs₃₀₀), absorption capability (MAE₃₀₀) of organic aerosols (Fig. 5). The Abs₃₆₅ and Abs₃₀₀ of organic aerosols were respectively 1.47 ± 0.96 and 4.34 ± 2.83 Mm⁻¹, and MAE₃₆₅ and MAE₃₀₀ were 0.43 ± 0.21 and 1.24 ± 0.38 m² g⁻¹ during the cruises. Light absorption parameters at 365 nm are more widely used in existing literature (Dasari et al., 2019). For some of our marine aerosol samples, however, the Abs₃₆₅ values were quite low or close to the detection limit, especially for the summertime samples, which could result in uncertainty for further analysis. Thus, we used the light absorption value at a wavelength shorter than 365 nm to investigate the BrC absorption properties and sources in marine atmospheres. Our previous work has suggested that the Abs₃₆₅ and Abs₃₀₀ of organic aerosols over the YBS displayed a similar variation trend (Zhang et al., 2025).

For the water-soluble organics, Abs₃₀₀ of WSOM displayed strong correlations with WSON concentration in the marine aerosols across seasons over the YBS (Fig. 5a). This revealed the importance of nitrogen-containing organic components for organic aerosol absorption. A strong dependence of WSOM absorption coefficient at 365 nm on WSON concentrations was also observed in atmospheric aerosols at inland city sites (Chen et al., 2026). However, for the water-insoluble fraction, we observed a strong correlation between Abs₃₀₀ of WIOM and WION only in the spring samples (Fig. 5b). For the autumn or summer cruises, we did not observe an obvious variation trend between WIOM Abs₃₀₀ and WION in the collected aerosol samples. This is consistent with our recent findings that absorption of brown carbon (BrC) over the YBS was generally dominated by water-soluble organics, and the contribution of water-insoluble organic aerosols increased during dust episodes (Zhang et al., 2025). Water-soluble organic nitrogen generally drove the light absorption by organic aerosols during non-dust periods over the YBS. During the spring dust period, both WSON and WION played important roles in the light absorption by marine organic aerosols over the East Asian marginal seas.

The elevated light absorption by organic aerosols was attributed not only to the higher ON concentrations but also to an increase in the absorption capability of organic aerosols. We plotted the variations of MAE₃₀₀ as a function of ON / OC ratios in Fig. 5c, d. For the summer samples, MAE₃₀₀ of WSOM showed an increasing trend as WSON / WSOC ratios increased (Fig. 5c). During the spring cruise, MAE₃₀₀ of WIOM elevated as the WION / WIOC ratios increased (Fig. 5d). Previous studies have concluded that organic molecules contributing to BrC absorption usually have a large degree of unsaturation and contain one or more nitrogen atoms (Laskin et al., 2015). These nitrogen-containing organic molecules are more prone to forming conjugated chromophores, thereby enhancing absorption by organic aerosols within the near-UV wavelength region (Laskin et al., 2015; Lin et al., 2016). For water-insoluble organic aerosols in autumn or summer, there was no clear variation trend in absorption capability with increasing WION / WIOC mass ratios (Fig. 5d). This was because light absorption of organic aerosols could also be contributed by non-nitrogenous chromophores (e.g., polycyclic aromatic hydrocarbons) in autumn or summer (Lin et al., 2018).

Variations of aerosol ON from continental and marine sources, as well as BrC absorption coefficients, are shown in Fig. 6 to understand the roles of ON from different sources in regulating the light absorption by marine organic aerosols. Continental WSON or WION includes those from dust-related formation, secondary nitrate formation, and aged biomass burning. Marine-generated WSON or WION includes those from marine biogenic emissions and sea spray aerosols. Samples during each cruise are listed in ascending order of continental WSON concentrations shown in Fig. 6a. The Abs₃₀₀ by WSOM or WIOM followed similar variation trends to the abundance of continental WSON or WION, and was different from that of marine-generated organic nitrogen (Fig. 6). Organic nitrogen compounds in marine-generated aerosols (e.g., amino acids, protein-like organic matters) are generally with low absorption within the UV to Vis wavelengths. Thus, marine-generated ON likely played a minor role in the organic aerosol absorption over East Asian marginal seas. Light absorption of WSOM showed a strong positive correlation (r=0.80) with continental WSON (inserted chart in Fig. 6a). This correlation also held within individual season (Fig. S10). The Abs₃₀₀ by WIOM displayed a consistent variation trend to continental WION, especially to the dust-related WION formation. As shown in the inserted chart in Fig. 6b, a strong positive correlation (r=0.73) was observed between Abs₃₀₀ by WIOM and dust-related WION formation. This clearly suggested the vital roles of transported continental aerosol ON in regulating the light absorption by organic aerosols over marginal seas. We used the mass ratio of Ca²⁺ / NO3- to roughly indicate the variation of relative contribution of dust and anthropogenic pollutants. The MAE₃₀₀ of WIOM, dominated by dust-related sources, displayed an increasing trend at a lower Ca²⁺ / NO3- mass ratio in spring (Fig. S11). This indicated that light absorption of dust-related organics would increase via interactions with anthropogenic pollutants (e.g., nitrate aerosols) during long-range transport through East Asia. This work provided observational evidence that aerosol ON from continental pollutants modulated the light absorption of marine organic aerosols over marginal seas. Our results are consistent with a recent modeling study, which emphasized the importance of biomass burning, anthropogenic emissions, and secondary formation for light-absorbing brown nitrogen on a global scale (Li et al., 2025b). What's more, our observation also emphasized the vital role of dust, through mixing with anthropogenic pollutants, in aerosol ON formation and light absorption during dust-storm season, which needs to be considered in the model.