A comprehensive sampling campaign was conducted at the regional background site Hok Tsui (HT, 22.20° N, 114.253° E) from 29 September to 18 November 2020. This site is situated on the southeastern tip of Hong Kong Island, facing the South China Sea. During the campaign, 31 valid daily fine particulate matter (PM2.5) samples were collected from 7 to 16 November 2020, using a high-volume sampler (TE-6070, TISCH, U.S) operating at a flow rate of approximately 1.0 m³ min⁻¹ (Table S1 in the Supplement). Prebaked quartz filters (450° for 5 h) were used to capture the particle matter, and the filters were subsequently wrapped in pre-baked aluminum foil after sampling. Field blank samples were also collected to ensure data accuracy. All samples were transported to the laboratory and stored at -20 °C prior to analysis.

A suite of online instruments was utilized to simultaneously measure gaseous pollutants and the chemical composition of particulate matter. To align with the PM_2.5 sampling periods, the online datasets were filtered for use in this study. HR-TOF-AMS was used to measure the composition of non-refractory submicron particulate matter (PM₁). Combing with the PMF method, four OA components were identified: a hydrocarbon-like OA (HOA), two less-oxidized oxygenated OAs (LO-OOA1 and LO-OOA2), and a more-oxidized oxygenated OA (MO-OOA) (Fig. S1 in the Supplement). Additionally, a TAG-TOF-MS was employed to measure organic markers, while a Proton Transfer Reaction time-of-flight mass spectrometer (PTR-TOF-MS) was applied to determine ambient concentrations of VOCs. Detailed information on the instrumental settings, calibrations, and data processing for HR-TOF-AMS (Huo et al., 2024a; Yao et al., 2022), TAG-TOF-MS (Huo et al., 2024b; Lyu et al., 2020), and PTR-TOF-MS (Yuan et al., 2024; Lyu et al., 2024) can be found in previous studies and is also briefly described in Supplementary text and Table S2. Furthermore, concentrations of PM_2.5, a series of trace gases (CO, NO, NO₂, O₃ and SO₂), and meteorological parameters (temperature, relative humidity) were continuously monitored.

The molecular composition of OAs in the offline PM_2.5 filters was analyzed using a high-resolution Q-Exactive Orbitrap mass spectrometer (Thermo Electron, Inc.) equipped with a heated electrospray ionization (ESI) source operating in negative mode. To address potential intermolecular suppression effects during ionization, an ultra-high performance liquid chromatography system (UHPLC, Dionex UltiMate 3000, Thermo Electron, Inc.) was employed for compound separation (Zhang et al., 2024; Thoma et al., 2022). Detailed descriptions of the analysis procedures and instrumental settings are available in the Supplement (Zhang et al., 2024; Wang et al., 2017b). Briefly, two pieces of PM_2.5 filters were punched using a stainless-steel puncher (Φ=20 mm), and the dissolved organic matter was extracted with 6 mL of mix-solvents (2×3 times, methanol : toluene = 1 : 1, v/v) using an ultrasonic cold-water bath for 20 min. The extracts were filtered through a 0.22 µm polytetrafluoroethylene membrane, combined, and evaporated to near dryness under a gentle stream of high-purity nitrogen. The residue was redissolved in 150 µL of methanol and centrifuged, with the supernatant transferred for subsequent HR-MS analysis. The scanning range of m/z was set from 50 to 800, with a typical mass resolution of 140 000 at m/z 200.

Non-target compound analysis was performed using the open-source software MZmine-2.37 (http://mzmine.github.io, last access: 29 June 2024). The analysis workflow included raw data import, peak detection, shoulder peak filtering, chromatogram building, chromatogram deconvolution, deisotoping, searching for adducts and peak complexes, alignment, gap filling, identification, and duplicate peak filtering (Wang et al., 2017b). Mass peaks were assigned to specific molecules with a mass tolerance of 2 ppm for ESI-mode. The molecular formulas were constrained to C_1–40H_0–100O_0–40N_0–5S_0–3, with additional criteria applied to elemental ratios (e.g., H/C, O/C) and double bond equivalents (DBE) to exclude chemically implausible formulas (Wang et al., 2017b; Lin et al., 2012). Elemental ratios, DBE, and modified aromatic index were calculated based on the assigned formulas of C_cH_hO_oN_nS_s, where c, h, o, n, and s are the number of carbon, hydrogen, oxygen, nitrogen and sulfur atoms, respectively. All reported molecules underwent blank subtraction, and those with an abundance ratio of less than 5 : 1 were excluded from the study (Ditto et al., 2018).

The EPA PMF5.0 model was employed to determine the relative contributions of different sources to the four AMS-PMF OAs. The mathematical framework of PMF has been described in detail in previous studies (Hopke, 2016; Norris et al., 2014). In brief, we used hourly concentration data of AMS-PMF OAs and SOA tracers as input for the EPA PMF model. While incorporating total OA mass along with chemical tracers in the PMF analysis can help distinguish the contributions of different sources to OA, it does not provide detailed source information for these AMS components, nor does it reveal how atmospheric conditions influence their oxidation states. The uncertainty ui,j for each species was calculated using the following equations: 1ui,j=xi,j×EF+(0.5×MDL)22(xi,j≥MDLs)2ui,j=5×MDL6(xi,j<MDLs) where xi,j denotes the concentration of species i in sample j, EF is the error fraction of each specie, and MDLs is the method detection limits for each species. Given that the concentrations of species used in PMF analysis can vary by orders of magnitude, applying the default error fraction may lead PMF to treat high concentration data as outliers, thereby reducing model robustness and increasing uncertainty in the results (Wang et al., 2017a). To address this issue, we adopted the error fraction of 0.2 for OA components and polar SOA tracers, and 0.3 for n-alkanes (Wang et al., 2019). The PMF model decomposes the xi,j matrix into factor profile (fk,j) and contribution matrices (gi,k) by minimizing the scaled residue (Q) based on the ui,j matrix. The optimal number of factors were preliminarily determined by examining the change in Qture/Qexp⁡ from 2–10 factors (Fig. S2). Bootstrapping (BS) was then applied to test the robustness of each solution, with factor matching rates above 80 % considered acceptable (Jiang et al., 2024). Ultimately, a six-factor solution was adopted, which showed good correlations between modeled and measured concentrations of each AMS-PMF derived OA component (r = 0.70–0.94), supporting the validity of using AMS-components as input variables.

The mathematical frameworks of PMF and NMF are virtually identical, with the key difference being that NMF only requires input values to be non-negative. Additionally, the error matrix required for EPA PMF analysis is typically unnecessary for NMF. These characteristics make NMF particularly suitable for factor decomposition of HR-MS data, where determining the detection uncertainty for each molecule is often challenging (Rund et al., 2023). The NMF routine was applied to the molecular composition data from the offline filter samples. However, we observed that compared to previous online TOF-MS analyses, the number of identified molecules using HR-orbitrap-MS increased significantly, reaching thousands, with some compounds sharing the same formulas but potentially having multiple sources. This complexity poses significant challenges for the interpretability of NMF factors. To address this, daily concentration data for the six factors obtained from the tracer-based PMF model were also used as constraints in the NMF model. This approach not only enhances the interpretability of NMF factors but also helps elucidate the molecular formation mechanisms underlying the PMF factors. Specifically, the contribution matrix of PMF factors was combined with the intensity-normalized data of HR-MS molecules to form a comprehensive input matrix, X. 3X∼G×F The NMF analysis was conducted using a R package “NNLM,” which tests the performance of 2–10 factors. The function of “nnmf” decomposes the input matrix X into two non-negative matrices, G and F, by minimizing the root-mean squared residual (RMSE) between X and its approximation, GF. Through this approach, both the percentages of PMF factors contributing to each NMF factor and the intensity fraction of each NMF factor relative to the total molecular intensity can be derived from the reconstructed matrix of GF. To determine the optimal number of factors, we plotted the variation of RMSE against the number of factors and selected the optimal value based on the Elbow rule (i.e., the point at which the RMSE reaches a minimum). We also calculated the global relevance between X and GF, following the method described by Rund et al. (2023), to identify the number of factors that best explain the variance. Furthermore, consensus cluster analysis was performed using the R package “ConsensusClusterPlus” (Monti et al., 2003) to further support the selection of the appropriate number of factors. By integrating all these evaluation criteria, we determined that five-factor was the optimal choice, as this was the smallest number that explained 99 % of the variance in the input data matrix (Fig. S3). It is noteworthy that the modeled factor concentrations showed good correlations with the input values, with average uncertainties ranging from 0.1 % to 1.5 %.

To assess the potential influences of regional transport on the composition of OAs during the sampling campaign, we used the National Oceanic and Atmospheric Administration (NOAA) Hybrid Single Particle Lagrangian Integrated Trajectory (HYSPLIT) model (https://www.ready.noaa.gov/HYSPLIT.php, last access: 1 July 2022) to calculate 120 h backward trajectories at 100 m heights using archived Global Data Assimilation System meteorological data (ftp://arlftp.arlhq.noaa.gov/pub/archives/gdas1, the link can only be opened using FTP software, last access: 1 July 2022). These hourly trajectories were clustered into three categories (C1–C3, Fig. S4) based on their origins and transport pathways. Category C3 (41 %) consisted of short-range continental air masses originating from central and northern China, reaching Hong Kong after traversing the Pearl River Delta (PRD) region. Category C2 (37 %) originated from North China and arrived in Hong Kong after passing through the East China Sea and coastal cities in southern China. The origins of Category C1 (22 %) could be traced to Mongolia, with air masses transported to Hong Kong along eastern and southern coastal cities. Additionally, a potential source contribution function (PSCF) analysis was conducted to evaluate possible source regions of PMF-derived source factors (Jiang et al., 2024). The PSCF analysis was performed using the open software MeteoInfo, with the 50th percentile of OA concentrations set as the threshold for PSCF calculations.

It should be noted that although our previous study (Huo et al., 2024a) reported AMS results, the differing time windows between the two studies may lead to different conclusions. To ensure consistency with the offline PM_2.5 samples analyzed in this study, only the AMS data corresponding to the same sampling period were selected and reanalyzed. Notably, even though the sampling campaign occurred during a period influenced by both continental and costal air masses from mainland China, the observed PM_2.5 concentrations remained relatively low (11–35 µg m⁻³, mean: 18 ± 5.0 µg m⁻³). This level was notably lower than historical urban measurements in Hong Kong (Wu et al., 2018). Yet, it still substantially exceeded the WHO guideline of 5 µg m⁻³. The reduction in PM_2.5 concentrations could be attributed to decreased anthropogenic emissions during the COVID-19 lockdown period (Huo et al., 2024a). Organic matter (OM = 1.8 × OC) (Gao et al., 2016) constituted 34 ± 16 % of the PM_2.5 mass, with its fractional contribution increasing to 52 ± 5.1 % in PM₁, as quantified by AMS (Fig. 1a), underscoring the critical role of OA in particulate matter formation. In our previous study, four OA components were identified in PM₁ using the AMS-PMF method throughout the sampling period, including one HOA and three OOA factors (Huo et al., 2024a). As shown in Fig. 1a, the temporal variation of OA concentrations was predominantly driven by LO-OOA1 (44 ± 12 %) and MO-OOA (32 ± 9.7 %), both influenced by regional transport, particularly LO-OOA1. For example, the highest OA concentrations were observed on the evening of 6 November, influenced by C3 air masses from central/northern China, with LO-OOA1 contributing up to ∼ 70 % of the OA, indicating regional transport as a potential driver of OA variation. For MO-OOA, back trajectory analysis revealed that air masses originating from continental China (C3) were associated with ∼ 17 % enhancements in MO-OOA concentrations (Fig. S4b). In contrast, HOA and LO-OOA2 exhibited limited temporal variation (each comprising ∼ 12 % of total OA) and varied less across air mass clusters, reinforcing their characterization as background OA components at this site. Our previous investigation identified photochemical processing as the dominant formation pathway for LO-OOA1 and MO-OOA compared to aqueous-phase reactions throughout the whole sampling period, evidenced by their differential correlation responses to oxidant levels and relative humidity (Huo et al., 2024a). In addition, photochemical reactions involving anthropogenic emissions have been shown to play a particularly important role in the formation of LO-OOA1, whereas MO-OOA is more influenced by biogenic emissions. However, during the focused sampling period in this study, LO-OOA1 exhibited strong associations with gas-phase photochemical reactions involving both biogenic and anthropogenic VOCs species, as well as NO_x (Fig. S5). In contrast, MO-OOA was more closely associated with SOA formation processes driven by ozone oxidation of BVOCs, as evidenced by strong correlations between MO-OOA and both O₃ and biogenic SOA tracers (r>0.50, p<0.01). For another OA component, LO-OOA2, only a limited number of species (e.g., hydroxyglutaric acids and adipic acid) showed good correlations with its concentrations, suggesting distinct secondary processes in its formation. Strong correlations were observed between HOA and anthropogenic species related to primary emissions, such as toluene, benzene/ethylbenzene fragments, NO_x and high-molecular-weight alkanes (> C₂₅). HOA was generally considered to relate to vehicle emissions. While vehicle emissions are important sources of benzene-like species and NO_x (Yuan et al., 2024), they predominantly emit low-molecular-weight alkanes (< C₂₆) (Geng et al., 2019; Fu et al., 2011). The high-molecular-weight alkanes are mainly derived from higher plants, but particles from primary biological emissions are typically in the coarse mode (Fu et al., 2011). Thus, our results suggest that HOA might also be influenced by anthropogenic emissions associated with biogenic materials, such as biomass burning or cooking. The presence of m/z 55, 57 and CO2+ in the mass spectra of HOA supports these speculations (Zhou et al., 2020).

To elucidate source-specific contributions to AMS-resolved OA components, we performed PMF analysis by integrating AMS-OA components, SOA tracers from TAG-TOF-MS, and VOC data from PTR-TOF-MS. Despite differences in particle cut-off sizes between AMS and TAG-TOF-MS, the AMS-derived OA mass was 110 % (62 %–230 %) of the OC/EC-based estimation in PM_2.5, confirming substantial organic matter enrichment in PM₁. The positive correlation between the results obtained from these two methods further supports the integration of the datasets (Fig. S6, r=0.54, p<0.01). This combined approach has been successfully applied in several previous studies to determine OA sources (Huo et al., 2024a; Huang et al., 2021). Based on the chemical species loading in each factor, we tentatively attributed the PMF-derived six factors to biomass burning related OA (BB-OA), cooking-related OA (C-OA), isoprene-derived SOA (Iso-SOA), monoterpene-derived SOA (MT-SOA), secondary inorganic aerosol-related OA (SIA-OA), and gas-phase photochemical SOA (gas-pSOA), respectively (Fig. S7). Figure 2c–i also presents the diurnal variations of OA concentrations contributed by each PMF factor.

The BB-OA and C-OA factors were predominantly composed of levoglucosan isomers (Simoneit, 2002) and oleic acid (Rogge et al., 1991), respectively. The OA concentrations from these factors exhibited similar diurnal patterns, peaking in the morning, declining during the daytime, and rising again in the evening (Fig. 2c–d). Notably, the C-OA factor also demonstrated high loadings of toluene and C8 aromatics, consistent with previous studies indicating that cooking processes can emit significant fractions of aromatic compounds formed through the cyclization of unsaturated fatty acids (Song et al., 2022, 2023). The two biogenic SOA factors, Iso-SOA and MT-SOA, were characterized by high loadings of 2-methylglyceric acid and C5-alkenetriols for Iso-SOA, and 3-methyl-1,2,3-butanetricarboxylic acid and Pinic acid for MT-SOA (Li et al., 2013a; Ding et al., 2016). The diurnal variations of OA contributed by these factors showed distinct patterns, with Iso-SOA peaking in the afternoon (14:00–15:00 LT) and MT-SOA reaching its highest values at noon, suggesting differences in their formation mechanisms. Comparisons with the diurnal variations of NO₂, O₃, and jNO₂ (the photolysis frequency of NO₂) suggest that Iso-SOA may be related to O₃ oxidation, whereas MT-SOA is associated with NO_x photocatalytic oxidation. Both factors showed positive correlations with temperature (r>0.50, p<0.01), consistent with previous studies indicating that elevated temperatures can enhance the emission of biogenic VOCs (Ding et al., 2016, 2011). The gas-pSOA factor exhibited high loadings of VOCs species, including photochemical products from both biogenic and anthropogenic species, supporting its association with gas-phase photochemical processes. This factor was less abundant in particle-phase SOA tracers, implying that gas-pSOA would produce less-oxidized or first-generation SOA products. The synchronous diurnal variation of gas-pSOA-contributed OA with O₃ suggested that gas-phase oxidation by O₃ was the main formation pathway, rather than oxidation by NO₂ photolysis (Fig. 2). SIA-OA was characterized by high loadings of nitrates, sulfates, and ammonium, along with anthropogenic SOA tracers such as m-/o-phthalic acid, hydroxylated benzoic acids, and low-molecular-weight alkanes (< C₂₆), suggesting influences from anthropogenic emissions such as biomass burning and vehicle emissions (Fu et al., 2011). The SIA-OA showed low values at noon but increased in the afternoon, peaking at 20:00, with a diurnal pattern similar to RH but opposite to jNO₂. As NO₂ photolysis weakens and RH increases, heterogeneous processes could promote the formation of SIA. Furthermore, nocturnal oxidation of VOCs initiated by the NO₃^⚫ radical and O₃ might be an important source of SIA-OA, as nighttime oxidation has been reported as a major pathway of SOA formation globally, particularly through NO₃^⚫ radical-initiated oxidation (Pye et al., 2010; Hoyle et al., 2007; Liu et al., 2024).

Figure 2a shows the time series of OA concentrations contributed by each factor. Overall, variations in OA concentrations during the sampling period were mainly associated with gas-pSOA, BB-OA, and SIA-OA, contributing 29 %, 22 %, and 20 % to the total OA, respectively. Biogenic SOA-related processes and C-OA accounted for 18 % and 11 % of OA, respectively. Figure 2b illustrates the contributions of PMF factors to each AMS-OA component. For LO-OOA1 and MO-OOA, which were the two main components driving OA variations throughout the sampling period, different contributions from SOA factors were evident. The combined contributions of gas-pSOA and BB-OA to LO-OOA1 exceeded 70 %, while SIA-OA's contribution was negligible. In contrast, the contribution of gas-pSOA to MO-OOA decreased to 21 %, with SIA-OA having the highest contribution to MO-OOA at 38 %, followed by biogenic SOA processes (Iso-SOA: 22 % and MT-SOA: 11 %). Therefore, the relatively higher oxidation degree of MO-OOA compared to LO-OOA1 could be attributed to greater contributions from SIA-OA and/or biogenic SOA processes. However, given that LO-OOA2 has an even higher proportion of SIA-OA (46 %) than MO-OOA, along with similar contributions from gas-pSOA, this suggests that the formation of highly oxidized organic compounds in MO-OOA might not be primarily driven by SIA-OA. Instead, it appeared to be more closely associated with biogenic SOA processes, particularly those involving Iso-SOA.

A PSCF analysis was conducted to identify the potential source regions for each OA factor obtained from the tracer-based PMF analysis during the sampling period. As shown in Fig. S8, one of the major source regions for BB-OA was central-northern China, including Henan and Shanxi provinces, where straw burning was an important source of PM_2.5 during the harvest season. Another source region for BB-OA was northern China and the Korean Peninsula, with fire maps (Fig. S9) indicating intense open BB activities in these regions during periods of elevated BB-OA. Southern China, including local emissions, was identified as a medium to high potential region for both biogenic SOA (Iso-SOA and MT-SOA) and C-OA, due to high biogenic emissions and cooking contributions in these regions (Zhang et al., 2025; Yao et al., 2021). However, coastal regions, including northern China and the Korean Peninsula, were also potential source regions for Iso-SOA, indicating that combustion-related sources might also play a significant role (Zhang et al., 2025). For OA related to gas-pSOA and SIA-OA, the medium to high potential source regions for gas-pSOA were coastal cities in eastern and southern China. In contrast, the potential source regions for SIA-OA also included northwestern China, such as Shanxi and Shaanxi provinces, where these regions often experienced high NO_x and SIA-OA concentrations due to anthropogenic emissions, e.g., coal combustion (An et al., 2019).

The integration of molecular tracers with AMS analysis provides an effective approach for elucidating the sources of OA, emphasizing the significant role of SOA processes in OA formation in South China. However, the molecular transformation mechanisms underlying the PMF-resolved factors, particularly for SOA, remain unclear. Thus, the molecular composition of OA was analyzed using an ESI-HPLC-HRMS based on offline daily PM_2.5 samples collected during the sampling period. A total of 10 012 unique molecular formulas were identified across all samples, among which CHO compound accounted for 30 ± 2.7 % of formular number, but their relative intensity was 67 ± 4.9 % (Fig. 3a). Correspondingly, CHON compounds accounted for 42 ± 6.1 % of the formular number, but their contribution to total intensity was only 15 ± 3.2 %. Additionally, the measured sulfur-containing organic compounds (CHOS+CHONS) accounted for 18 ± 5.4 % of the total intensity. Unlike many studies conducted in mainland China, which are substantially influenced by anthropogenic emissions or liquid-phase reactions, high proportions of nitrogen-containing or sulfur-containing compounds were frequently observed (Li et al., 2024; Han et al., 2023; Zhang et al., 2024; Jiang et al., 2023). Nitrogen-containing or sulfur-containing compounds are typically considered anthropogenic primary emissions or classes of relatively stable compounds in SOA that related terminal oxidation for oxygenated OA under high-NO_x conditions (Han et al., 2023; Fan et al., 2022; Jiang et al., 2023). In fact, as the NO_x concentration during the entire sampling period was less than 10 % of O₃, our results may indicate that the oxidation processes cannot effectively transform the oxygenated OA into nitrogen-containing or sulfur-containing compounds.

Previous studies have indicated that ESI- is more inclined to detect oxidized and polar compounds (Lin et al., 2012; Jiang et al., 2016). Figures 3b–d and S10 show the molecular distribution of compound groups detected in this study. Among the detected CHO compounds, C8–12 species are the most abundant, accounting for over 50 % of the total intensity. Several high-intensity compounds, such as C₈H₁₂O₄₋₆, C₈H₁₀O₅, C₉H₁₄O₅₋₆, and C₁₀H₁₆O₅ have been commonly detected in laboratory simulation studies and environmental samples and are considered monoterpene-SOA components (Table S3) (Romonosky et al., 2015; Xu et al., 2021). However, compounds with the same molecular formulas have also been identified in biomass burning aerosols (Wang et al., 2017c) and SOA derived from aromatic oxidation (Mehra et al., 2020; Kumar et al., 2023). In this study, positive correlations were observed not only between these compounds and biogenic species (Fig. S11) but also with anthropogenic VOCs and SOA tracers, indicating their multiple sources. Even if these compounds were derived from the oxidation of biogenic VOCs, the influence of anthropogenic emissions could not be ruled out, as biomass burning and cooking are also important sources of biogenic VOCs (Zhang et al., 2025; Song et al., 2022). The intensities of these compounds were positively correlated with typical tracers for cooking and its atmospheric oxidation products (i.e., oleic and azelaic acids) (Xu et al., 2023; Bikkina et al., 2014), but not with levoglucosan, supporting the potential origins from cooking for these compounds. Due to the lack of corresponding structural information, it is challenging to determine the specific sources of these compounds.

It is important to note that the oxidation of aromatic VOCs is an important source of OA in this study. A series of anthropogenic-related compounds were detected in our samples, exhibiting high abundance, such as C₇H₆O₂, C₈H₆O₄, and C₇H₁₀O₅. Additionally, abundant CHON compounds were detected, with C₆–C₁₀ nitroaromatic compounds dominating the total intensity. Nitroaromatic compounds are widely observed in environmental aerosols and are primarily derived from the oxidation of anthropogenic-related VOCs, particularly those associated with biomass burning OAs (Xie et al., 2017; Li et al., 2019; Cai et al., 2022). Overall, molecular-level analysis based on offline HR-MS data indicated that secondary SOA formation from both anthropogenic and biogenic emissions was the main source of OA during the study period. This highlights the complex interplay between different emission sources and the transformation processes contributing to OA composition.

Although previous source apportionment methods using molecular composition data from various online mass spectrometers (e.g., EESI-TOF-MS) have been widely applied to determine the source of OA (Ge et al., 2024), these methods have primarily focused on specific fractions of OA, such as CHO and CHON compounds, due to their importance as precursors of particle SOA (Zheng et al., 2023; Ge et al., 2024). To further understand the impact of PMF-resolved sources and SOA processes on OA formation at the molecular level, a constrained-NMF model was applied by simultaneously incorporating the six PMF factors and the molecules identified by HR-MS analysis. It is noteworthy that while the hourly concentrations of each PMF factor are independent, significant correlations were found between the daily-average concentrations of MT-SOA, Iso-SOA, and C-OA, aligning with the time windows of PM_2.5 samples. As a result, an independent MT-SOA factor could not be obtained in our constrained-NMF model (Fig. 4), as it was mainly shared by the NMF factors of Iso-SOA and C-OA (referred as Iso-SOA_NMF and C-OA_NMF, same for other factors). However, the model effectively distinguished the BB-OA, gas-pSOA, and SIA-OA factors resolved by tracer-based PMF model. Overall, the five-factor solution explained over 99 % of the total variance, allowing for the identification of molecules associated with each tracer-based PMF factor. It should be noted that the mass spectra of all factors resolved by the constrained-NMF model might differ from those of source samples or laboratory-generated SOA, as our results primarily reflected the characteristics of each tracer-based PMF factor observed in the real ambient atmosphere (Mo et al., 2024). The compounds identified in each NMF factor may not fully correspond to the names of the PMF factors, as PMF factors represent not only specific sources but also indicate that certain compounds may share similar formation pathways with the atmospheric processes implied by the factor names. For example, in the Iso-SOA_NMF factor, many anthropogenic-related compounds might also be present alongside biogenic SOA, suggesting that these anthropogenic compounds could have similar atmospheric formation pathways as biogenic SOA.

Figure 4 presents the mass spectra for each factor obtained from the constrained-NMF analysis, with several highly intense species also indicated. As shown in Table S4, which summarizes the average chemical parameters of each NMF factor, the C-OA_NMF was featured by the highest O/C ratio and the lowest DBE value. Within this factor, a series of highly abundant compounds, including C₈H₁₂O₅, C₈H₁₀O₅, C₈H₁₂O₄, C₉H₁₄O₅, C₈H₁₂O₆, C₁₀H₁₆O₅ and C₉H₁₄O₆, were observed. As previously mentioned, these compounds may originate from the oxidation of monoterpenes emitted from both biological sources and cooking. Previous studies have suggested that although alkanals, alkenals, and alkadienals are identified as the main types of emissions from cooking, their proportion in household cooking emissions in China is relatively small. This indicates that the precursors and SOA formed from cooking oil heating emissions may not fully represent the precursors and SOA formed from real-world cooking emissions (Yu et al., 2022; Song et al., 2022). A recent study has shown that even during the cooking process of fried foods, emissions of oleic acid and linoleic acid are relatively low compared to aromatic hydrocarbons (Song et al., 2022, 2023). Therefore, the presence of some high-abundance aromatic compounds, such as C₇H₆O₂, in this factor is reasonable. Additionally, oxygen-containing compounds, especially short-chain acids and aldehydes (i.e., hexanoic acid, hexanal, and nonanal), are abundant in cooking vapor. These short-chain acids can react with SO₂ in the atmosphere to form organosulfates (Passananti et al., 2016; Zhu et al., 2019), which explains the high abundance of C6 organosulfate compounds observed in the C-OA_NMF factor. Notably, we also observed a high abundance of C₁₀H₁₇NSO₇, a typical nitrooxy organosulfate generated by the atmospheric oxidation of monoterpenes (Surratt et al., 2008).

The Iso-SOA_NMF exhibited an O/C ratio similar to that of C-OA_NMF but had the highest effective oxidation number (nO_eff) values among all NMF factors (Table S4). This observation supports our earlier speculation that the elevated oxidation level of MO-OOA in AMS-PMF derived OA components could be attributed to significant contributions from Iso-SOA. In addition to several highly intense monoterpene SOA species, a series of C₅ oxygen-containing compounds, such as C₅H₆₋₈O₄ and C₅H_6–8O₅, also displayed high intensity in the Iso-SOA_NMF factor (Fig. 4). However, due to the lower ionization efficiency of ESI- for compounds with fewer than six carbon atoms (Kebarle and Tang, 1993), the abundance of these C₅ compounds is not as high as that of C_6–8 compounds.

The BB-OA_NMF factor showed the lowest O/C and H/C ratios but the highest DBE and AI values compared to other NMF factors (Table S4), indicating its high aromaticity. This factor contained not only monoterpene SOA but was also rich in oxygen-containing aromatic compounds (e.g., C₇H₆O_2–3, C₈H₈O₃, and C₈H₆O_4–5). These compounds are potential phenolic substances that may originate from the pyrolysis of lignin (Siemens et al., 2023; Kawamoto, 2017; Lin et al., 2016). Importantly, the mass spectrum of this factor included a large fraction of nitrogen-containing compounds, particularly nitrophenols (e.g., C₆H₅NO₃, C₆H₅NO₄, C₇H₅NO₅, and C₈H₇NO₅). Nitrophenols have been widely reported in both fresh and aged biomass burning OAs, primarily formed by the reaction of phenolic compounds from lignin pyrolysis with inorganic nitrogen (Li et al., 2019; Lin et al., 2017; Song et al., 2018).

The gas-pSOA_NMF factor contained a high abundance of aromatic-CHO compounds, nitroaromatic compounds, and CHOS compounds (Fig. 4). The chemical processes involved in gas-phase reactions are relatively complex. On one hand, the high abundance of C8–C10 aromatic-CHO compounds may result from the photo-oxidation of PAHs (Keyte et al., 2013), and some nitroaromatic compounds can also be generated through gas-phase photochemical reactions (Cai et al., 2022; Fan et al., 2022). Given the high RH during the sampling period, the uptake of SO₂ by VOCs in the gas phase is a primary pathway for the generation of organosulfates (Bruggemann et al., 2020; Ye et al., 2018). Although the atmospheric SIA formation processes are also complex and may partially overlap with gas-pSOA processes, gas-phase oxidation (both daytime ^⚫OH oxidation and nighttime NO₃^⚫ oxidation) remains a major formation pathway for SIA (Zhu et al., 2023). Our results indicated that sulfur additions were less significant compared to gas-pSOA processes. As mentioned earlier, we found that variations in SIA-OA were potentially affected by the nocturnal oxidation of VOCs (NO₃^⚫/O₃ oxidation). Notably, nighttime organic nitrates generally formed through reactions between NO₃^⚫ and alkenes in the gas phase, with NO₃^⚫ adding to the double bond of unsaturated VOCs to generate alkene-like organic nitrates (Ng et al., 2017; Fan et al., 2022). A higher proportion of alkene-like CHON compounds was observed in the SIA-OA_NMF (21 %) compared to the gas-pSOA_NMF factor (8 %), with the compound C₉H₁₇NO₃ (DBE = 2) showing the highest average intensity in SIA-OA_NMF. These findings collectively support the influence of nocturnal oxidation on the formation of SIA-OA.

Figure 5 illustrates the relative abundance of molecules identified by the PMF factor-constrained NMF method as a proportion of the total identified compounds. Notably, the contributions of biogenic SOA, cooking and BB to OA derived from the molecular composition-based NMF analysis aligned with the results from the tracer-based PMF model. However, the contribution of gas-pSOA to OA from the NMF method was 1.4 times that of the PMF model, while the contribution of SIA-OA to OA was only 1/3 of the PMF model's estimate. Although the tracer-based PMF model can mathematically separate atmospheric SOA processes into SIA and gas-pSOA, these categories may still partially overlap in real-world conditions. As discussed above, gas-phase oxidation, particularly nocturnal oxidation, is a major pathway for SIA formation. Our results suggest that, in the NMF analysis, many compounds associated with SIA processes may have been over-attributed to gas-pSOA, potentially leading to an underestimation of the contribution of nocturnal oxidation to SOA formation. However, given the relatively stable levels of SIA-OA observed during the sampling period, and considering that misclassification between SIA-related and gas-pSOA-related species did not affect the contributions from other sources (BB, biogenic SOA, and cooking) or the total SOA contributions, the results from the molecule-based NMF analysis remain reasonably robust. Importantly, both methods consistently indicated that gas-phase oxidation of VOCs was a significant pathway for OA formation throughout the study period, particularly for anthropogenic VOCs. This is evidenced by the relative abundance of potential aromatic compounds (DBE ≥ 4), which ranged from 45 % to 61 % in the NMF factors, highlighting the substantial impact of anthropogenic emissions on OA formation in this study.