Highly time-resolved chemical speciation and source apportionment of organic aerosol components in Delhi, India, using extractive electrospray ionization mass spectrometry
- 1Laboratory of Atmospheric Chemistry, Paul Scherrer Institute, 5232 Villigen PSI, Switzerland
- 2Department of Environmental Science, Stockholm University, Stockholm, Sweden
- 3Geosciences Division, Physical Research Laboratory, Ahmedabad 380009, India
- 4Department of Civil & Environmental Engineering, University of Illinois at Urbana-Champaign, Urbana, Illinois 61801, United States
- 5Centre for Atmospheric Sciences, Indian Institute of Technology Delhi, New Delhi 110016, India
- 6Department of Civil Engineering and Centre for Environmental Science and Engineering, Indian Institute of Technology Kanpur, Kanpur 208016, India
- anow at: Department of Chemistry and Applied Biosciences, ETH Zurich, 8093 Zurich, Switzerland
- bnow at: Department of Environmental Studies, University of Delhi, Delhi 110007, India
- cnow at: Department of Civil and Infrastructure Engineering, Indian Institute of Technology Jodhpur, Jodhpur 342037, India
- dnow at: Tofwerk AG, Uttigenstrasse 22, 3600 Thun, Switzerland
Correspondence: Sachchida N. Tripathi (firstname.lastname@example.org), André S. H. Prévôt (email@example.com), and Jay G. Slowik (firstname.lastname@example.org)
In recent years, the Indian capital city of Delhi has been impacted by very high levels of air pollution, especially during winter. Comprehensive knowledge of the composition and sources of the organic aerosol (OA), which constitutes a substantial fraction of total particulate mass (PM) in Delhi, is central to formulating effective public health policies. Previous source apportionment studies in Delhi identified key sources of primary OA (POA) and showed that secondary OA (SOA) played a major role but were unable to resolve specific SOA sources. We address the latter through the first field deployment of an extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF) in Delhi, together with a high-resolution aerosol mass spectrometer (AMS). Measurements were conducted during the winter of 2018/19, and positive matrix factorization (PMF) was used separately on AMS and EESI-TOF datasets to apportion the sources of OA. AMS PMF analysis yielded three primary and two secondary factors which were attributed to hydrocarbon-like OA (HOA), biomass burning OA (BBOA-1 and BBOA-2), more oxidized oxygenated OA (MO-OOA), and less oxidized oxygenated OA (LO-OOA). On average, 40 % of the total OA mass was apportioned to the secondary factors. The SOA contribution to total OA mass varied greatly between the daytime (76.8 %, 10:00–16:00 local time (LT)) and nighttime (31.0 %, 21:00–04:00 LT). The higher chemical resolution of EESI-TOF data allowed identification of individual SOA sources. The EESI-TOF PMF analysis in total yielded six factors, two of which were primary factors (primary biomass burning and cooking-related OA). The remaining four factors were predominantly of secondary origin: aromatic SOA, biogenic SOA, aged biomass burning SOA, and mixed urban SOA. Due to the uncertainties in the EESI-TOF ion sensitivities, mass concentrations of EESI-TOF SOA-dominated factors were related to the total AMS SOA (i.e. MO-OOA + LO-OOA) by multiple linear regression (MLR). Aromatic SOA was the major SOA component during the daytime, with a 55.2 % contribution to total SOA mass (42.4 % contribution to total OA). Its contribution to total SOA, however, decreased to 25.4 % (7.9 % of total OA) during the nighttime. This factor was attributed to the oxidation of light aromatic compounds emitted mostly from traffic. Biogenic SOA accounted for 18.4 % of total SOA mass (14.2 % of total OA) during the daytime and 36.1 % of total SOA mass (11.2 % of total OA) during the nighttime. Aged biomass burning and mixed urban SOA accounted for 15.2 % and 11.0 % of total SOA mass (11.7 % and 8.5 % of total OA mass), respectively, during the daytime and 15.4 % and 22.9 % of total SOA mass (4.8 % and 7.1 % of total OA mass), respectively, during the nighttime. A simple dilution–partitioning model was applied on all EESI-TOF factors to estimate the fraction of observed daytime concentrations resulting from local photochemical production (SOA) or emissions (POA). Aromatic SOA, aged biomass burning, and mixed urban SOA were all found to be dominated by local photochemical production, likely from the oxidation of locally emitted volatile organic compounds (VOCs). In contrast, biogenic SOA was related to the oxidation of diffuse regional emissions of isoprene and monoterpenes. The findings of this study show that in Delhi, the nighttime high concentrations are caused by POA emissions led by traffic and biomass burning and the daytime OA is dominated by SOA, with aromatic SOA accounting for the largest fraction. Because aromatic SOA is possibly more toxic than biogenic SOA and primary OA, its dominance during the daytime suggests an increased OA toxicity and health-related consequences for the general public.
Atmospheric aerosols are suspensions of tiny solid or liquid particles in the air, ranging from a few nanometres (nm) to tens of micrometres (µm) in size. Aerosols can affect climate directly by scattering (including reflection) and absorbing solar radiation, thereby altering the radiative balance of the earth–atmosphere system, and indirectly by acting as cloud condensation nuclei (CCN), thereby affecting the number and lifetime of clouds (Forster et al., 2007). Aerosol particulate matter with an aerodynamic diameter less than or equal to 2.5 µm (PM2.5) can easily be deposited deep into human lungs and induce oxidative stress and inflammation, leading to various cardiovascular and respiratory diseases (Pope et al., 2009; Salvi, 2007; Shiraiwa et al., 2017). Aerosols can be composed of various species such as mineral dust and soluble inorganic species such as nitrate, sulfate, ammonium, and chloride, as well as organic and elemental carbon. It is estimated that organic aerosols (OAs) can account for 20 % to 90 % of the total fine particulate mass (Jimenez et al., 2009). OA is classified as either primary OA (POA), which is directly emitted into the atmosphere, or secondary OA (SOA), which is produced in the atmosphere by the oxidation of volatile organic compounds (VOCs) emitted from anthropogenic or natural processes, producing lower-volatility products which form new particles or condense onto the pre-existing aerosols. In many areas, SOA accounts for a substantial portion of total OA mass (Jimenez et al., 2009). However, despite SOA being an important fraction of total OA and its toxicity (Daellenbach et al., 2020), our understanding of sources and formation processes of SOA in the atmosphere remains incomplete (Hallquist et al., 2009; Shrivastava et al., 2017). This limits our ability to accurately constrain SOA contributions in global climate models and regional air quality models and impedes efforts to understand SOA health effects.
Delhi, the capital city of India, is a growing megapolis with a population of about 17 million and a population density of 11 320 persons km−2 as per the most recent census, conducted in 2011 (Planning Department; Government of NCT of Delhi, 2021). It experiences high levels of air pollution and is amongst the most polluted cities in the world, with an annual mean PM2.5 concentration of ∼140 µg m−3 (World Health Organization, 2018), which is much higher than the Indian National Ambient Air Quality Standard (NAAQS) of 40 µg m−3 for annual PM2.5 concentration (Central Pollution Control Board, 2009). During the post-monsoon season, severe air pollution events are frequent, with PM2.5 levels often reaching as high as 1000 µg m−3 (Sembhi et al., 2020). Several recent studies have investigated the composition and sources of non-refractory (NR) OA in Delhi using highly time-resolved online measurements by an aerosol mass spectrometer (AMS) or an aerosol chemical speciation monitor (ACSM) (Bhandari et al., 2020; Gani et al., 2019; Lalchandani et al., 2021; Tobler et al., 2020). These studies were able to quantitatively resolve the most dominant POA sources, i.e. traffic-related, hydrocarbon-like organic aerosol (HOA) and biomass burning organic aerosol (BBOA) (Bhandari et al., 2020; Lalchandani et al., 2021; Tobler et al., 2020). However, they were not able to assign specific sources to the oxygenated organic aerosol (OOA), due to the use of thermal volatilization (∼600 ∘C) in combination with harsh electron impact ionization (EI, ∼70 eV) for ion generation in the AMS and ACSM, which results in substantial fragmentation of analyte molecules and loss of molecular information. Generally, while AMS and ACSM datasets provide quantitative estimates of individual POA factors and total SOA contribution, they are able to describe SOA only in terms of bulk descriptors such as the level of oxygenation (i.e. bulk O:C ratio).
To overcome these limitations on fragmentation and thermal decomposition, several offline continuous and semi-continuous instruments have been developed. The offline techniques provide a high degree of chemically specific information with the possibility of molecular identification as well. They, however, have low time resolution (typically hours to ∼1 d) and include possible artefacts from reactions or partitioning on the surface (Pospisilova et al., 2020; Zhao et al., 2018). Among the continuous and semi-continuous techniques, for example, the chemical analysis of aerosol online particle inlet coupled to a proton transfer reaction time-of-flight mass spectrometer (CHARON-PTR-MS) employs an aerodynamic particle lens for sampling and a thermal desorption unit for volatilization of aerosol constituents, which are then ionized using a proton transfer reaction (PTR) ionization scheme and analysed by a mass spectrometer. Although a proton transfer reaction mass spectrometer (PTR-MS) has a softer ionization scheme than EI, the energy remains high enough to yield substantial fragmentation of organic analytes (Eichler et al., 2015; Müller et al., 2017). The Filter Inlet for Gases and AEROsols (FIGAERO) coupled to a high-resolution time-of-flight chemical ionization mass spectrometer (HR-TOF-CIMS) is a semi-continuous system where aerosol particles are first collected onto a polytetrafluoroethylene filter. The particle-laden filter is then analysed periodically by passing heated ultra-high-purity nitrogen gas through the filter. The resulting vapours are ionized by chemical ionization mass spectrometry, e.g. with iodide adducts (Lopez-Hilfiker et al., 2014). Although FIGAERO uses a soft ionization technique, some compounds are still affected by thermal decomposition (Stark et al., 2017) and reactions of analytes on the filter (Kristensen et al., 2016). Moreover, it has a lower time resolution (>30 min) compared to online techniques (≤ 1 min).
Finally, a novel extractive electrospray ionization (EESI) interface was coupled to a portable high-resolution time-of-flight mass spectrometer (EESI-TOF) (Lopez-Hilfiker et al., 2019). The EESI-TOF enables highly time-resolved measurements of a wide range of atmospherically relevant oxygenated compounds, including sugars, alcohols, acids, and organonitrates (Lopez-Hilfiker et al., 2019; Stefenelli et al., 2019) with detection limits on the order of 1–10 ng m−3. The EESI-TOF detection limits are sufficient to measure these compounds with a 5 s time resolution under typical ambient conditions with negligible thermal decomposition, ionization-induced fragmentation, or matrix effects. The EESI-TOF provides the near-molecular-level information (i.e. molecular formula) with a lack of direct structural information. This is a clear limitation of 1-D mass spectrometric techniques such as the EESI-TOF, AMS, and CHARON-PTR, as opposed to the chromatographic separation and tandem MS approaches possible in the offline analysis. In addition to that, different molecules exhibit different relative sensitivities in systems like the EESI-TOF (Lopez-Hilfiker et al., 2019; Wang et al., 2021). Recent field studies in Europe and China have demonstrated the advantage of the chemical resolution of the EESI-TOF for source apportionment of ambient OA (Qi et al., 2019; Stefenelli et al., 2019; Tong et al., 2021).
Here, we deployed an AMS and an EESI-TOF for 2 weeks in Delhi and report comprehensive source apportionment results from the AMS and EESI-TOF datasets with a time resolution of ∼10 min. We utilized the quantitative power of the AMS and the higher chemical resolution of the EESI-TOF to derive quantitative estimates of individual sources of SOA and report the results from the first-ever deployment of the EESI-TOF in Delhi. Having a quantitative estimate of individual SOA contributing factors is a valuable advancement in understanding and predicting the SOA health effects and its formation mechanisms and devising effective mitigation policies.
2.1 Campaign overview and sampling site
To understand and analyse the chemical composition and sources of various components of submicron PM in Delhi, we conducted a wintertime campaign in South Delhi at the Indian Institute of Technology Delhi (IITD) campus (28.54∘ N, 77.19∘ E) from 31 December 2018 to 14 January 2019. A suite of particle- and gas-phase instrumentation was deployed which included an extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF) for conducting time-resolved measurements of the organic aerosol molecular ions; a high-resolution aerosol mass spectrometer (HR-AMS) for measuring non-refractory PM1 (NR-PM1) composition; a scanning mobility particle sizer (SMPS), consisting of a model 3080 differential mobility analyser (DMA) and model 3022 condensation particle counter (CPC) (TSI, Inc., Shoreview, MN, USA) to measure the particle size distribution from 15.7 to 850.5 nm; an Aethalometer (model AE33, Magee Scientific, Ljubljana, Slovenia) to measure the equivalent black carbon (eBC) concentration; and an Xact 625i Ambient Metals Monitor (Cooper Environmental Services LLC, Tigard, OR, USA) to measure the mass of 35 different elements in PM10 and PM2.5 separately (Rai et al., 2020).
All instruments were housed in a temperature-controlled laboratory (22 ∘C) on the top floor of a four-storey building (∼12 m high) housing other laboratories and faculty offices. Aerosol sampling was performed through stainless-steel tubing (6 mm i.d., 8 mm o.d.) of ∼3 m length. A PM2.5 cyclone (BGI, Mesa Labs, Inc.) was installed at the inlet of the sampling line to remove larger particles. Here, we have used the co-located measurements by the HR-AMS and the EESI-TOF with the supporting data from other instruments as required. More details on the operation of the EESI-TOF and the HR-AMS are given in the following sections.
The sampling site, i.e. IITD's location, is representative of the Delhi urban area. The nearest source of local emissions is an arterial road located ∼150 m away from the building, and there are also emissions from residential use of solid fuels for cooking and heating and biomass burning in the nearby areas. A detailed description of this site's location as well as its demographic and geographic details is provided elsewhere (Lalchandani et al., 2021; Rai et al., 2020; Singh et al., 2021; Wang et al., 2020).
2.2.1 Extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF)
The use of the EESI-TOF allows continuous and highly time-resolved measurements of organic aerosol composition on a near-molecular level (i.e. chemical formulae of molecular ions) with negligible thermal decomposition or ionization-induced fragmentation. A detailed description of the EESI-TOF and its operating principles has been provided elsewhere (Lopez-Hilfiker et al., 2019). Briefly, the sampled aerosols first pass through a multi-channel charcoal denuder to strip gaseous components. Breakthrough of gas-phase species can cause high background signals, as previously observed in Beijing (Tong et al., 2021). In that study, a small denuder (diameter of 4 mm and length of 30 to 40 mm) was used, whereas in the present study we used a larger denuder (i.e. with 69 channels, outer diameter 8.5 mm, length 60 mm). The denuder was exchanged every 48 h and regenerated by baking at ∼200 ∘C for 12 h. The denuder was positioned ∼20 cm upstream of the electrospray and mass spectrometer inlet to avoid decreased transmission of larger particles (Tong et al., 2021). After passing through the denuder, the sampled particles intersect with a plume of electrospray (ES) droplets generated by a commercial electrospray probe and delivered through a fused silica capillary with precut tips with an inner diameter of 50 µm (BGB Analytik AG). The ES solution used in this study consisted of a 1:1 water acetonitrile () mixture doped with 100 ppm NaI. The ES solution was charged by applying a high potential difference (∼2.5–2.7 kV) at the ES capillary tip. The flow of ES solution through the silica capillary is controlled by a high-accuracy microfluidic flow controller (Fluigent GmbH). Upon intersection with ES droplets, the soluble fraction of analyte aerosol is extracted into the droplets. The analyte-laden droplets then pass through a heated stainless-steel capillary (∼250 ∘C), wherein the electrospray solvent evaporates, and analyte ions are generated. Due to the short residence time (∼1 ms) in the capillary, heat transfer to the particles is limited, and negligible thermal decomposition is observed. Finally, the ions are analysed by a high-resolution long-time-of-flight mass spectrometer (LTOF-MS, Tofwerk AG, Switzerland) configured for positive ion detection. In the configuration of the mass spectrometer and ionization scheme used in this study, one can detect a wide range of molecules present in the organic aerosols, including sugars, alcohols, acids, and organonitrates. The detected molecular classes include nearly all the compounds present in the secondary organic aerosol (SOA), with notable exceptions of organosulfates, which are typically detected as negative ions, and non-oxygenated species such as alkanes and alkenes. The mass resolution () achieved by the mass analyser in this study was ∼8000. This resolution is enough to separate isobars (compounds with same nominal mass) and determine the molecular formula. Due to the lack of direct structural information, the molecular assignments given here are, however, tentative and may include contributions from multiple isomers. The ions were observed predominantly as adducts with Na+, i.e. [M]Na+, but for simplicity are denoted herein using the neutral formula (M). For example, an ion observed as [C6H10O5]Na+ is reported as C6H10O5.
The EESI-TOF sampled continuously at a flow rate of ∼1 L min−1, alternating between direct ambient sampling (5 min) and sampling through a particle filter (3 min) for measurement of the instrument background. This measurement–filter cycle is shorter than those used in previous ambient measurements to avoid clogging of the EESI capillary and to increase the spray stability. The EESI-TOF data analysis was performed using Tofware version 2.5.7 (Tofwerk AG, Switzerland). The original data were acquired at a time resolution of 1 Hz, and high-resolution (HR) peak fitting was applied to data averaged to 10 s for the mass-to-charge ratio () range 145–350. In total, 1030 ion formulae were fitted. The ambient aerosol composition (Mdiff) was calculated by subtracting background spectra obtained during particle filter sampling (Mfilter) from the mass spectra obtained during direct ambient sampling (Mtotal). The background spectra (Mfilter) were calculated by interpolating the average between adjacent background spectra (i.e. particle filter measurements before and after an ambient sampling period). This methodology is similar to the one reported in previous EESI-TOF studies (Qi et al., 2019; Stefenelli et al., 2019; Tong et al., 2021). After obtaining the ambient aerosol composition, the ambient aerosol spectra (Mdiff) were averaged to 10 min for further processing. The error matrix (σdiff) corresponding to Mdiff values was calculated from Poisson ion counting statistics (Allan et al., 2003) from ambient sampling σtotal(i,j) and filter sampling periods σfilter(i,j), added in quadrature as follows:
As a final step, data were filtered to remove ions whose total signal and/or variability was either dominated by the background or too noisy for meaningful interpretation. Ions that met both of the following criteria were accepted for further analysis:
The ratio of signal to uncertainty, i.e. , was considered, where σdiff represents the precision-based uncertainties as calculated by using Eq. (1). Ions with a median were removed from further analysis (Paatero and Hopke, 2003).
The ratio of signal to background, i.e. , was considered. This identifies ions whose time series is dominated by instabilities in the spray and/or background drifts due to adsorption/desorption of semi-volatile compounds. Ions with a median ratio of were removed.
In the end, 641 ions between ranges of 150–350 were retained for further analysis.
2.2.2 High-resolution time-of-flight aerosol mass spectrometer (HR-AMS)
The HR-AMS (Aerodyne Research Inc., Billerica, MA, USA) was equipped with a PM1 aerodynamic lens and measured the composition of NR-PM1. A detailed description is given elsewhere (DeCarlo et al., 2006; Canagaratna et al., 2007). Briefly, ambient air is sampled continuously through a critical orifice into a PM1 aerodynamic lens, which focuses the particles into a narrow beam and accelerates them to a velocity that is inversely related to their vacuum aerodynamic diameter (Williams et al., 2013). The particles then impact a resistively heated surface (∼600 ∘C) and flash vaporize. The resulting gas is ionized by electron impact ionization (EI, 70 eV) and detected by a time-of-flight mass spectrometer. The detected ion rate measured at a specific mass-to-charge ratio () is then converted to mass concentration in µg m−3 (Jimenez et al., 2003).
In this study, two ionization efficiency (IE) calibrations of the instrument were performed (one before the commencement of the campaign and the other at the end) using 300 nm NH4NO3 particles. More details on the instrument operation during this campaign have been reported elsewhere (Singh et al., 2021, 2019). The instrument was operated in V mode at a time resolution of 2 min. Every 30 s, it switched between mass spectra (MS) and particle time-of-flight (PToF) mode, completing two cycles within each integration period. The mass spectra of an ensemble of particles are measured in MS mode, whereas in the PToF mode, the particle beam is modulated by a chopper spinning at 130 Hz, resulting in the size-resolved mass spectra. Unit mass resolution (UMR) data were analysed using the SQUIRREL data analysis toolkit (version 1.59) programmed in the Igor Pro 6.37 software environment (WaveMetrics, Inc., Portland, OR, USA). High-resolution peak fitting analysis was conducted using PIKA (version 1.19) (DeCarlo et al., 2006) for 12 to 120. The collection efficiency was estimated using the composition-dependent algorithm of Middlebrook et al. (2012) implemented in SQUIRREL. The Pieber correction was applied according to the method recommended by Pieber et al. (2016).
2.3 Source apportionment
2.3.1 Positive matrix factorization
Source apportionment was performed separately on the AMS OA and EESI-TOF datasets using the positive matrix factorization (PMF) algorithm (Paatero and Tapper, 1994) implemented within the multilinear engine (ME-2; Paatero, 1999). In this study, the Source Finder Professional (SoFi Pro 6.8, Datalystica Ltd.) interface was used for model configuration and post-analysis (Canonaco et al., 2013). PMF is a bilinear model that represents the sample matrix X with dimensions of m×n, representing m measurements of n variables as a product of two matrices G (dimensions of m×p) and F (dimensions of p×n). The number of columns in the modelled matrix G and rows in the modelled matrix F are equal to the number of factors p, i.e. individual sources chosen to describe the dataset. The PMF model operates under non-negativity constraints; i.e. negative values are not permitted in G or F. The PMF model is expressed as
Here G represents the time-dependent factor concentrations (i.e. time series) and F represents the chemical composition (i.e. mass spectrum) of the resolved factors. Model residuals are contained in E.
The PMF model solves Eq. (2) using a least-squares algorithm that iteratively minimizes the objective function Q, defined as
In Eq. (3), eij represents elements of the residual matrix and σij represents the measurement uncertainties corresponding to the input point xij, where i and j are the indices representing measurement time and variable (or integer ), respectively. The theoretical value of Q, denoted Qexp, can be estimated as
PMF is subject to rotational ambiguity, meaning that different combinations of G and F matrices exist that can yield the same or similar Q values. Some of these combinations may represent environmentally unreasonable representations of the dataset. To direct the model towards interpretable rotations, a priori information can be introduced by constraining selected factor time series or mass spectra using an a-value approach (Canonaco et al., 2013; Crippa et al., 2014). In this method, one or more factor profiles and/or time series are constrained to resemble reference profiles and/or time series, with the scalar a () determining the tightness of constraint. As an example, if constraints are applied to mass spectra, the a value determines the extent to which a factor mass spectrum in the final solution (fj,solution) is allowed to deviate from the anchor mass spectrum (fj) provided to the model as the initial starting point.
As an example, if an a value of 0.1 is used, all the variables in the resulting mass spectrum can vary between ± 10 % of the input constraining the mass spectrum. Note that post-PMF normalization of factor profiles may cause the final values to slightly exceed the limits defined by Eq. (5).
2.3.2 Source apportionment of AMS dataset
The AMS OA matrix XAMS consisted of organic ion time series derived from high-resolution (HR) peak fitting for 12 to 120 and the integrated signal across integer (unit mass resolution or UMR) for 121 to 300. A total of 507 variables were used in the sample matrix XAMS, 332 of which had chemical formulae assigned to them through HR fitting. The remaining 175 variables were UMR species. For the UMR data, we excluded 149 due to interference from phthalic acid emitted by the servo housing, as well as 183, 184, and 186 due to the interference from the tungsten filaments. Uncertainties were calculated according to the method by Allan et al. (2003), which accounts for counting statistics of the individual ions as well as the uncertainty in the detector response to individual ions. Variables with a signal-to-noise ratio (SNR) <0.2 were downweighted by a factor of 10, whereas those with an SNR <2 were downweighted by a factor of 2 (Paatero and Hopke, 2003). Further, ions calculated from the CO signal (i.e. O+, OH+, H2O+, and CO+) were removed from XAMS prior to PMF analysis to avoid overweighting CO intensity (Ulbrich et al., 2009) and were recalculated from CO during post-analysis. Note that this remove-and-reinsert strategy is preferable to downweighting of CO-dependent ions as it avoids the potential for small biases induced by the combination of AMS minimum errors and dynamic downweighting in “robust mode” operation of the PMF.
As a first step, we ran the PMF in unconstrained mode with the number of factors ranging from 3 to 8. Each solution was inspected based on its value and physical interpretation of individual factors. Large decreases in the values were observed when the number of factors increased from 3 to 5, while small incremental changes were observed when the number of factors increased beyond 5. Further, solutions with more than 5 factors yielded only additional biomass-burning-related factors, the differences between which could not be physically interpreted. Hence we chose a 5-factor solution as the best representation of the data. The unconstrained PMF resulted in an HOA factor with a high degree of oxygenation, i.e. O:C ratio ∼ 0.15, which is a factor of ∼3 higher than the HOA factor obtained at the same site in a recent study (Lalchandani et al., 2021). To obtain a cleaner HOA profile, we took the HOA factor profile from an unconstrained 8-factor solution and used it in SoFi to constrain the HOA factor in the final 5-factor solution. We explored the PMF solutions with higher numbers of factors, but the O:C ratio of the HOA profile did not show a significant decrease for solutions with more than 8 factors.
The factors obtained from the AMS source apportionment were identified based on their correlations with external measurements, mass spectral features, diurnal trends, and relationship to anthropogenic activities as well as meteorological and environmental conditions (e.g. temperature, expected trends in human activities). The interpretation of the final 5-factor solution is discussed in Sect. 3.1.
2.3.3 Source apportionment of EESI-TOF dataset
A total of 641 ion formulae from 140–350 were used in the final PMF input matrix XEESI of the EESI-TOF data. The initial PMF model was run without constraints for 6 to 15 factors, and each solution was checked for the interpretability of the results. The 6-factor solution yielded a factor identified as primary biomass burning (characterized by ∼90 % of factor profile signal from C6H10O5, which is likely dominated by levoglucosan, a biomass burning tracer), and 5 other factors related to primary cooking emissions, aged biomass burning, and 3 SOA factors (described in Sect. 3.2). Although the main spectral and temporal features of these factors were not consistent with primary biomass burning, they nonetheless contained significant signals from C6H10O5 (comprising 10 %–15 % of the factor profiles), consistent with mathematical mixing of biomass burning into these factors. Increasing the number of factors from 6 to 10 decreased the contribution of C6H10O5 in the aged biomass burning factor to ∼12 %, consistent with similar factors observed in previous studies (Qi et al., 2019; Tong et al., 2021). For the non-biomass-burning factors, the contribution of C6H10O5 to the factor profiles decreased to <2.5 %, while key spectral and temporal features were retained. As the number of factors increased, the newly added factor profiles all had high (>20 %) contributions from C6H10O5, which is characteristic of primary biomass burning. However, these new factors could not be physically interpreted and were therefore considered to result from mathematical splitting. Increasing the number of factors to 11–15 yielded only further splitting of the primary biomass burning profiles and no longer affected the C6H10O5 contributions to the non-primary biomass burning factors.
This preliminary analysis suggested that the variability in the dataset is optimally represented by 6 factors. However, because the unconstrained 6-factor solution did not provide unmixed factors (as described above), we constructed an unmixed 6-factor solution by constraining profiles for primary cooking, aged biomass burning, and the 3 SOA factors. The reference profiles used in SoFi for these 5 factors were taken from the unconstrained 10-factor solution. The remaining five profiles (from the unconstrained 10-factor solution) were combined on a mass-weighted basis to form a single primary biomass burning profile. This 6-factor solution is referred to as the “base case” hereafter.
The statistical stability of and uncertainties in the base case were accessed by a combined bootstrap analysis–randomized a-value selection (i.e. sensitivity test of the tightness of constraint). Bootstrapping was implemented by random resampling of the rows of the original data matrix and corresponding entries of the error matrix, such that in each bootstrap iteration some rows were sampled multiple times while others were not sampled at all, thus creating new matrices in each iteration of the bootstrap analysis that were of the same dimensions as the original input matrices (Davison and Hinkley, 1997; Paatero et al., 2014). Simultaneously the a values of the 5 constrained factors (primary cooking-related, aged biomass burning, and 3 unique SOA factors) were randomly selected from within predefined limits chosen to maximize exploration of the solution space while maintaining computational efficiency. The bootstrap–a-value analysis was conducted in two stages: (1) an exploratory analysis on a small number of runs that was used to determine the a-value limits and (2) the final analysis on 1000 bootstrap runs with a-value randomization occurring within these limits.
The a-value limits for the combined bootstrap–a-value randomization analysis were selected after an exploratory analysis of 250 bootstrap runs in which the a values of every constrained factor were allowed to vary over the full range (0 to 1), with a step size of 0.1. The 250 individual solutions were analysed and classified as “good” or “mixed” following the method of Stefenelli et al. (2019), which consists of the following steps: (1) calculation of the Spearman correlation coefficients between the time series of each factor from the base case and a bootstrap solution, yielding a correlation matrix for each bootstrap run with the correlation values between bootstrap factors and corresponding base case factors on the matrix diagonal; (2) requirement that the correlation coefficient on the matrix diagonal was higher than those on the intersecting row and column by a statistically significant margin (based on a preselected significance level p from a t test). Solutions satisfying this requirement were classified as good solutions, whereas those failing this test were classified as mixed solutions. From visual analysis of ∼50 randomly selected solutions, we selected p=0.3 as the appropriate confidence level. We then assessed the acceptance probability as a function of a value, selecting the a-value upper boundary to be the value above which 75 % of solutions were classified as mixed. The ranges of a values selected for cooking-related OA and 4 SOA factors are given in Supplementary Table S1.
The a-value limits obtained above were utilized in a final combined bootstrap–a-value randomization analysis, consisting of 1000 runs. Solutions resulting from this 1000-run bootstrap were separated into good and mixed solutions using the same acceptance/rejection criteria as used in the exploratory bootstrap. The final bootstrap analysis resulted in 835 good solutions out of 1000 that were kept for further analysis. The solution presented in Sect. 3 is the average of these 835 solutions.
2.4 Estimation of the fraction attributable to local production or emissions during daytime
In order to isolate the effects of boundary layer dynamics and gas–particle partitioning from those of photochemical production, we modelled the average concentration of all EESI-TOF factors during the daytime (averaged between 10:00 to 16:00 local time (LT)) (denoted Cmodel) based on the average concentration of the previous night (averaged between 21:00 and 04:00 LT), assuming that all changes were driven by partitioning and/or boundary layer expansion. The dilution and partitioning effects on the SOA factors were calculated by attributing each factor to a distinct organic species with bulk properties as given in the Supplementary Table S2. The relative difference between measured (Cmeasured) and modelled average daytime concentrations (Cmodel) is attributed to local photochemical production for SOA factors and local emissions for POA factors. This analysis was applied to each factor on a day-by-day basis.
The modelled daytime concentration of a particular factor on a day i, Cmodel,i, was calculated by combining the effects of both dilution and partitioning on the average nighttime concentration, , of that factor observed during the previous night (i.e. day i − 1):
where Df is the dilution factor, i.e. the fractional change in nighttime concentrations due to dilution, and Pf is the partitioning factor, i.e. the fractional change in the nighttime concentrations due to gas–particle partitioning.
The dilution factor for each day was calculated using the ratios of planetary boundary layer heights (PBLHs) during the nighttime and daytime. PBLH data were obtained from the Real-time Environmental Applications and Display sYstem (READY; Rolph et al., 2017) website. The PBLH data were available at a 3 h resolution; hence single values of PBLH obtained at 00:00 during the nighttime and 12:00 during the daytime were used for each day.
The partitioning coefficient ξp for each factor p was calculated using basic partitioning theory:
where COA is the mass concentration of organic aerosols (measured OA mass by AMS in this study) and c∗ is the effective saturation vapour concentration of each factor. The activity coefficient was assumed to be 1 (Donahue et al., 2006). The saturation vapour concentration at room temperature, c∗ (298 K), was estimated using the molecular corridor approach (Li et al., 2016), based on the framework developed originally for the two-dimensional volatility basis set (Donahue et al., 2011):
where is the reference carbon number; nC and nO are the number of carbon and oxygen atoms, respectively, which are given in supplementary Table S2; bC and bO are the corresponding parameterization values for each class of compounds (i.e. CH and CHO); and bCO is the coefficient of carbon–oxygen non-ideality, ), hereafter referred to as NICO. The , bC, bO, and bCO values used were 25, 0.475, 0.2, and 0.9, respectively (Mohr et al., 2019; Tröstl et al., 2016; Pankow and Asher 2008). The temperature-dependent effective saturation concentration c∗(T) was calculated using the Clausius–Clapeyron equation (Li et al., 2016; Donahue et al., 2006). ξp was calculated for each factor on an hourly basis and was later averaged to obtain single daytime and nighttime values for each day. The partitioning factor Pf was calculated by using Eq. (9):
Based on modelled daytime concentration (Cmodel) and observed daytime concentration (Cmeasured), the fraction of daytime concentrations attributed to local photochemical production for SOA factors or to direct emissions for POA factors was calculated using the following equation:
3.1 AMS source apportionment results
From the AMS source apportionment, we identified three primary factors, namely hydrocarbon-like OA (HOA) and biomass burning OA (BBOA-1 and BBOA-2), and two secondary factors, denoted more oxidized oxygenated OA (MO-OOA) and less oxidized oxygenated OA (LO-OOA). Figure 1 shows the factor mass spectra (Fig. 1a), time series (Fig. 1b), and diurnal trends (Fig. 1c) of all factors. The relative contributions of these factors to total OA mass on a 24 h basis, during the daytime and during the nighttime, are shown by means of pie charts in Fig. 1d.
The HOA mass spectrum contains prominent contributions from CxH fragments (e.g. C3H, C3H, C4H, C3H). This is consistent with saturated and unsaturated hydrocarbons, which are major constituents of fossil fuels. Similar factors have been observed in many previous studies and are typically associated with traffic emissions (Lanz et al., 2007; Zhang et al., 2011). The diurnal pattern (Fig. 1c) shows a small peak during the morning rush hour (07:00 LT) and a larger one during the evening rush hour (18:00–22:00 LT). The morning peak is partially obscured by the decreasing concentrations due to dilution caused by a rising boundary layer. As a result, the HOA factor reaches its minimum during midday hours (12:00–16:00 LT). Such strong boundary layer cycling is a known characteristic of Delhi and affects nearly all primary species (Gani et al., 2019; Lalchandani et al., 2021; Tobler et al., 2020). The low temperatures during the evening hours reduce the boundary layer height, resulting in an accumulation of species. The HOA time series is well correlated with NOx, further supporting the assignment of this factor to traffic-related sources, as shown in Fig. 1b.
The mass spectra of both BBOA-1 and BBOA-2 have strong signals from C2H4O ( 60) and C3H5O ( 73) fragments, which are characteristic fragments of anhydrosugars like levoglucosan (Aiken et al., 2009), a product of cellulose pyrolysis (Hoffmann et al., 2010; Simoneit et al., 1999). The high abundances of these fragments in BBOA mass spectra have been reported in earlier studies (Crippa et al., 2013; Zhang et al., 2011). BBOA-1 has about 1.5 % and 0.8 % of its total signal attributed to C2H4O and C3H5O, respectively, compared to 3.9 % and 1.7 %, respectively, for BBOA-2. All other factors have lower contributions from these fragments; HOA, MO-OOA, and LO-OOA have 0.3 %, 0.2 %, and 0.8 % of their total signal, respectively, attributed to C2H4O, and 0.2 %, 0.1 % and 0.4 % of their total signal, respectively, attributed to C3H5O. BBOA-1 and BBOA-2 explain 21.6 % and 36.8 % of the temporal variability in C2H4O, while LO-OOA, MO-OOA, and HOA explain 20.3 %, 11.6 %, and 3.1 %, respectively, of its temporal variability. Similarly, for C3H5O, BBOA-1 and BBOA-2 explain 20.9 % and 31.6 % of its temporal variability, respectively, while LO-OOA, MO-OOA, and HOA explain 20.2 %, 17.8 %, and 4.3 % of its temporal variability, respectively. The rest is unexplained variability. The BBOA factors also have higher contributions (relative to other factors) from high species, e.g. 116, 118, 202, which were previously associated with polycyclic aromatic hydrocarbons (PAHs) (Bruns et al., 2015; Dzepina et al., 2007).
The bulk O:C, H:C, and N:C ratios of BBOA-1 are 0.37, 1.8, and 0.05, respectively, compared to 0.47, 1.84, and 0.019 for BBOA-2. The N:C value is almost 2.5 times higher for BBOA-1 compared to BBOA-2. A nitrogen-rich solid-fuel combustion factor was identified in a previous study at the same site and was attributed to biomass combustion with possible mixing of coal and other solid fuels (Lalchandani et al., 2021). Both BBOA-1 and BBOA-2 show similar diurnal trends with an evening time increase, indicating increased emissions as well as a reduction in boundary layer height due to decreasing temperature (Gani et al., 2019; Lalchandani et al., 2021), and very low values during daytime hours. A steep decline during midday hours of both BBOA-1 and BBOA-2 is attributed to less intense source contributions and an increase in boundary layer height as well as the increased volatilization of semi-volatile components. A contrasting feature in diurnal trends of BBOA-1 and BBOA-2, however, is the extent to which both these factors increase in the evening hours as compared to their average daytime values. While BBOA-1 increases by a factor of ∼2–3 during the evening hours, BBOA-2 increases by a factor of ∼10 during the same time. The differences in bulk elemental ratios and diurnal patterns of the BBOA factors support their treatment as separate factors.
The primary biomass burning and aged biomass burning factors from the EESI-TOF (see Sect. 3.2) also show a similar trend, with the diurnal pattern of the primary biomass burning factor from the EESI-TOF showing an increase of a factor of ∼50 during the evening rush hours, whereas the oxidized biomass burning factor only exhibits a ∼2–3-fold increase during the same time (Fig. S1 in the Supplement).
From the two retrieved SOA factors, MO-OOA is more oxygenated with a bulk O:C ratio of 0.99, which is the highest among all the factors (>2 times higher than that of LO-OOA and BBOAs and ∼12 times higher than HOA). The mass spectrum of MO-OOA contains large contributions from CO), consistent with OOA factors described in other studies (Ng et al., 2010). The CO fragment usually arises from carboxylic acid groups in diacids or multifunctional acidic compounds (Duplissy et al., 2011). The high degree of oxygenation suggests its secondary origin (Jimenez et al., 2009; Zhang et al., 2011). Despite the aforementioned boundary layer effects, the diurnal trend of MO-OOA shows an increase during the day, implying formation occurs as a result of daytime photochemical reactions, although the sources or precursors cannot be inferred from the AMS factor spectrum. Overall, MO-OOA correlates well with SO measured by the AMS.
LO-OOA contains a lower contribution from CO (though still higher than any of the POA factors) and higher contributions from less oxygenated species. The bulk O:C ratio of this factor is 0.46. Due to the lower oxygenation and presumably higher volatility of LO-OOA, its partitioning behaviour between the gas and particle phase is more sensitive to the ambient temperature and the total OA concentration than MO-OOA. As a result, LO-OOA exhibits increased concentrations at night (lower temperature, higher total OA).
The PMF analyses on the AMS dataset as discussed above show the relative importance of primary and secondary sources (Fig. 1d) with traffic and primary biomass burning as major contributors to the primary organic aerosol. However, while the AMS can quantify total SOA and delineate it by the extent of oxygenation and/or volatility, it does not provide source-specific information. In the next section, we report the source apportionment results from EESI-TOF data and investigate the individual sources that could contribute to the SOA factors.
3.2 EESI source apportionment results
The EESI-TOF source apportionment results yielded six factors. Of these, biomass burning and cooking-related OA were attributed to primary aerosol. The remaining four factors were attributed to secondary sources and denoted aromatic SOA, biogenic SOA, aged biomass burning, and mixed urban SOA. These EESI-TOF factors can be qualitatively related to the AMS, with EESI-TOF primary biomass burning corresponding to AMS BBOA and the four EESI-TOF secondary factors providing a more source-specific representation of AMS OOA (i.e. MO-OOA + LO-OOA). Note that cooking-related OA was retrieved only by the EESI-TOF and not the AMS (see discussion below), while as expected the EESI-TOF did not retrieve HOA due to its insensitivity to alkanes and alkenes (see Sect. 2.2.1). Related AMS and EESI-TOF factors are compared below as appropriate.
3.2.1 Primary factors
Primary biomass burning
The mass spectrum of primary biomass burning is dominated by C6H10O5, likely associated with anhydrosugars such as levoglucosan, mannosan, and galactosan. C6H10O5 constitutes 81.1 % of the total mass spectral signal in this factor (Fig. 2a). The second-highest contribution to the mass spectrum comes from the ion C8H12O6 (2.1 % of the total signal), which could possibly be a derivative of syringol, a prominent compound found in wood-burning smoke (Yee et al., 2013). These features are qualitatively similar to primary biomass burning mass spectra observed by EESI-TOFs in previous studies (Qi et al., 2019; Stefenelli et al., 2019; Tong et al., 2021). The next three highest contributing ions with 0.47 %, 0.44 %, and 0.33 % of total signal are C11H14O4, C6H12O5, and C6H10O4, respectively. C11H14O4 could be tentatively assigned to syringyl ethanone, whereas C6H10O4 may be associated with methylglutaric acid. Both of these compounds have previously been found in biomass burning smoke (Bertrand et al., 2018; Qi et al., 2019).
The time series of the primary biomass burning factor observed by the EESI-TOF (Fig. 2b) correlates strongly with the summed time series of the two BBOA factors from AMS (r=0.85). The diurnal trend of this factor shows a distinct peak during the evening rush hours between 18:00–22:00 LT and thereafter a steady decline throughout the night with an early morning rise starting between 05:00–06:00 LT and peaking at 08:00 LT before decreasing to low values during midday hours (12:00–16:00 LT) (Fig. 2c). The diurnal trend is also qualitatively similar to the AMS HOA and BBOA factors, in that the time of early morning rise coincides with an increase in anthropogenic activities. Another observation is that during the daytime (12:00–16:00 LT) the primary biomass burning declines to less than 4 % of its average concentrations from the previous night. Three effects might drive these very low daytime concentrations of primary biomass burning: first, the decline in source intensities; second, the strong dilution effects from boundary layer expansion; and third, increased evaporation of semi-volatile constituents due to higher temperature and the aforementioned dilution. The primary biomass burning factor constitutes on average around 70 % of the total EESI-TOF OA signal, whereas the AMS BBOA factors contribute on average 44.7 % to the total organic mass measured by the AMS. This is due to the higher sensitivity of the EESI-TOF towards levoglucosan as compared to most other classes of compounds, as consistently observed in laboratory and field studies (Lopez-Hilfiker et al., 2019; Stefenelli et al., 2019; Tong et al., 2021). (Note that the EESI-TOF insensitivity to HOA cannot explain this discrepancy, as AMS BBOA contributes only 50.9 % of the non-HOA organic mass, i.e. .)
A notable feature in the mass spectrum of this factor is that ∼9.2 % of the total signal in this factor comes from ions with H:C ratios >1.7 and O:C <0.25. The contribution of such ions to biogenic SOA is 5.0 %, with all other factors falling below 2.1 %. The carbon number distribution of these ions is shifted towards higher carbon numbers, consistent with saturated and non-saturated fatty acids (see Fig. 3). Such molecules are prominent constituents of cooking oils (Orsavova et al., 2015). The high relative contributions from such species are consistent with previous cooking-related factors resolved in EESI-TOF studies (Tong et al., 2021; Qi et al., 2019).
The time series of cooking-related OA explains a large fraction of the signal from ions consistent with fatty acids, e.g. 32.1 %, 38.8 %, 34.6 %, and 33.9 % of C16H32O2, C16H30O2, C18H34O2, and C18H36O2, respectively. The other five factors combined explain only 15 %–20 % of the variation in these fatty-acid-like compounds, while the rest remains unexplained; ∼5 %–10 % is explained by residuals and ∼90 %–95 % by noise. Figure S3 shows the fractional contribution of all EESI-TOF factors to the diurnal trends of two selected fatty-acid-like compounds, tentatively attributed to oleic acid (C18H34O2) and stearic acid (C18H36O2). As one can clearly see, the cooking-related OA factor is the dominant contributor to these species, regardless of time of day or ion concentration. This observation of the high contribution of cooking-related factor to observed diurnal patterns of fatty-acid-like compounds is also consistent with previously defined cooking-related OA factors from the EESI-TOF (Tong et al., 2021; Qi et al., 2019).
The diurnal trend of cooking-related OA shows qualitatively similar features to primary biomass burning, in that it decreases during daytime hours and peaks during the late evening (Fig. 2c). Cooking-related OA increases by a factor of ∼6 from 16:00–19:00 LT, remaining roughly stable till 00:00 LT, followed by a decline till 06:00 LT, and then remaining approximately stable until 10:00 LT. During the day, a small peak is observed during lunchtime (13:00–15:00 LT), which may indicate active sources in the vicinity of the measurement site. The average day-to-night ratio is approximately a factor of 10 higher than that of primary biomass burning, which further supports the possibility of active sources during the day.
We note that no cooking-related factor was identified in the AMS PMF results. The unconstrained PMF analysis yielded an HOA factor with high levels of oxygenated fragments, especially the oxygenated fragments at 55 and 57, which might indicate mixing of cooking-related factor into HOA. However, it is also possible that these oxygenated fragments were contributed by some other sources (e.g. BBOA or LO-OOA); hence a definite conclusion on the mixing of the cooking-related factor into unconstrained HOA could not be drawn. Neither constraining a COA profile from the literature in the AMS PMF nor increasing the number of factors up to 15 yielded cooking-related factors. Possible reasons for this may be the similarity of the cooking-related OA spectrum with the HOA and BBOA spectra in the AMS, high relative concentrations of the other primary factors, and strong effects of boundary layer dynamics on the diurnal patterns of all factors (leading to collinearity among unrelated factors), all of which combine to make it difficult to separate a relatively minor cooking-related factor without the specific tracer ions provided by the EESI-TOF.
3.2.2 Secondary factors
The mass spectrum of this factor has ∼63.0 % of its total signal contributed by compounds with six to nine carbons (C6−C9). A large fraction of this comes from molecules with an H:C ratio <1.5 (27.9 % of the total signal from C6−9HyOz ions and 7.1 % from C6−9HyOzN1−2 ions) (Fig. 3). As a comparison, biogenic SOA, aged biomass burning, and mixed urban SOA have an 11.7 %, 27.2 %, and 18.3 % contribution from C6−9HyOz ions and 4.0 %, 2.9 %, and 3.7 % contribution from C6−9HyOzN1−2 ions with H:C ratios <1.5, respectively. The low H:C ratios are associated with aromatic systems, as the precursor gases are highly unsaturated and contain fewer hydrogen atoms than more saturated straight-chain or ring-containing compounds. In a recent study on the source apportionment of VOCs at the same site, it was found that aromatic C6−9Hy VOCs constitute 45.4 % of total VOC loading and are emitted into the atmosphere predominantly from anthropogenic activities, of which traffic constituted the highest fraction during the daytime (Wang et al., 2020). Oxidation of these aromatic VOCs is most likely the dominant process leading to the formation of this factor.
In order to substantiate the claim that the major ions contributing to the ambient aromatic SOA factor are indeed formed by oxidation of aromatic VOCs, we conducted a chamber experiment in the Paul Scherrer Institute (PSI) smog chamber using a mixture of aromatic compounds consisting of benzene, toluene, ethylbenzene, and trimethylbenzene (Kumar et al., 2022). These compounds are well-established constituents of vehicular emissions (Cao et al., 2016; Yao et al., 2015) especially for gasoline vehicles during the cold start phase (Platt et al., 2017). OH radicals were produced in the chamber and reacted with the VOCs, resulting in the formation of SOA, whose chemical composition was subsequently compared with the aromatic SOA and other SOA factors obtained in this study.
Figure S2 shows the mass spectrum of the ambient aromatic SOA factor colour-coded by ions that were found in chamber SOA formed from oxidation of aromatics. Approximately 32.0 % of the EESI-TOF signal contained in the aromatic SOA factor overlapped with ions identified in the chamber experiment. This signal fraction is considerably higher than for other SOA factors, i.e. biogenic SOA, aged biomass burning, and mixed SOA had signal contributions from chamber SOA ions of 16.0 %, 26.0 %, and 20.0 %, respectively.
Despite the strong dilution of the boundary layer during the day, there is little variation in the aromatic SOA concentration during the day. This points to a strong local daytime source, such that the production of aromatic SOA is fast enough to offset the strong dilution effects of the expanding boundary layer as discussed further in Sect. 3.5.
The mass spectrum of biogenic SOA is shown in Fig. 2a. It contains high contributions from ions such as C9H16O5, C8H14O6, and C9H14O4, which have been previously identified in EESI-TOF factors representing biogenic oxidation products (Qi et al., 2020; Stefenelli et al., 2019). Compounds with H:C >1.5 constitute nearly 50 % of the signal of this factor, with 2.9 %, 5.0 %, 6.8 %, and 2 % of signal resulting from C7H10−14O4−8, C8H12−16O4−8, C9H14−18O4−8, and C10H16Oz, respectively. These compounds have been previously attributed to monoterpene oxidation products in Zurich, Switzerland (Stefenelli et al., 2019). There are, however, some notable differences from the Zurich study. Specifically, the present study shows a much smaller contribution from the C10H16Ozcompounds (6.2 % in Zurich vs. 2 % in this study), while CxHyOzN1 compounds comprise 26.7% of the factor profile (vs. ∼13% in Zurich). These differences might arise because of two different reasons. One is the probable contribution of not only monoterpene oxidation products (which dominate in Zurich) but also isoprene oxidation products, e.g. C5H10Ox and C5H9NOx (Chen et al., 2020), to the biogenic factor retrieved in this study. This is because of Delhi's location near the tropics, which results in a large contribution of isoprene to the total biogenic VOCs. Model estimates predict isoprene emission fluxes to be a factor of ∼20 higher than α-pinene in tropical regions of India, whereas in Europe the emission fluxes of isoprene and monoterpenes are similar (Guenther et al., 2012; Sindelarova et al., 2014). Zurich and Delhi also differ in terms of atmospheric conditions, in particular the much higher NOx levels in Delhi as compared to Zurich, consistent with the higher CxHyOzN1 fraction. Biogenic VOCs such as monoterpenes and isoprene are susceptible to oxidation by NO3 radicals, which can result in large amounts of biogenic SOA production. In Delhi, however, due to large concentrations of NO (∼200–300 ppbv) during the nighttime, the production of NO3 radicals is suppressed and the diurnal cycle of NO3 is actually inverted with the majority of available NO3 radicals actually present during the daytime (Haslett et al., 2022).
The diurnal trend of this factor resembles that of the EESI-PMF primary factors in that the concentration is highest overnight and a strong decrease is seen during daytime hours. A possible explanation of this behaviour could be more regional sources of the biogenic VOCs scattered over a large area. This means that the biogenic SOA factor most likely has only a small daytime source in the vicinity of the site.
Aged biomass burning
The fractional contribution of levoglucosan (C6H10O5) to the aged biomass burning factor mass spectrum is ∼10 %, which is a factor of 8 lower than for the primary biomass burning factor. The lower levoglucosan content in the aged biomass burning mass spectrum as compared to the primary biomass burning mass spectrum is consistent with observations of similar factors in Zurich during winter (Qi et al., 2019). Additionally, chamber studies have shown that the levoglucosan concentration decreases in aged biomass burning particles (Bertrand et al., 2018), while the concentrations of secondary species increase, consistent with observations in this study.
The mass spectrum of this factor also has ∼2 % contributions each from two key ions, C6H8O6 and C7H8O7. These are most likely oxidation products of phenols and methoxy-phenols, which are abundant secondary compounds formed during the ageing of biomass burning emissions (Yee et al., 2013) and are important precursors of biomass burning SOA. The aged biomass burning factor contains dominant signals from various other small molecules with H:C ratios less than 1.3, which is consistent with the oxidation of small aromatic compounds emitted during biomass burning such as phenolic compounds. These compounds were observed to be major contributors of gas-phase solid-fuel combustion factors in a recent VOC source apportionment study conducted at the same site (Wang et al., 2020).
The diurnal trend of aged biomass burning is similar to the one of primary factors, characterized by increased concentrations during evening hours and a decline during daytime hours. The amplitude of the evening time peak however differs between aged biomass burning and primary biomass burning (Fig. S1). While the primary biomass burning increases by a factor of ∼50–60 between 17:00–22:00 LT, the increase in oxidized biomass burning is within a factor of ∼5 during the same time. Between 22:00–07:00 LT, the concentration of this factor steadily decays by a factor of 2.5. A distinct peak is also observed between 07:00–09:00 LT, which coincides with an increase in solar radiation, indicating that ageing of emissions takes place during early morning hours. Note that it is likely that a majority of local emissions are not oxidized during nighttime in Delhi due to very high levels of NO (∼200–300 ppb), which may scavenge both O3 and NO3 radicals during nighttime and inhibit nocturnal degradation of VOCs (Haslett et al., 2022).
The diurnal pattern of the LO-OOA factor from AMS correlates well with the aged biomass burning factor from the EESI-TOF and suggests that oxidation of biomass burning emissions may be the dominant contributor to the LO-OOA factor observed in the AMS.
Mixed urban SOA
The remaining factor is most likely a mixed SOA factor, which has influences from both anthropogenic and biogenic sources. The highest-intensity ions in this factor are C5H10O4, C9H14O5, C6H10O5, C9H16O5, C9H18O5, and C6H12O4. C5H10O4 is probably a product of isoprene oxidation, whereas the dominance of C9 compounds suggests contributions from oxidation products of C9 species. The C9 species have varied sources in urban areas which include evaporative losses of fuels (e.g. gasoline), solvent use, and unburnt exhaust emissions (Mehra et al., 2020; Zhang et al., 2013), and hence this factor is likely influenced by different sources linked to the Delhi urban area. This factor also has ∼2.5 % of mass spectral signal contributed by levoglucosan (C6H10O5). Either this could be due to non-perfect unmixing by PMF, or it could indicate the contributions from biomass burning with other above-mentioned sources in this factor. This factor is therefore named mixed urban SOA.
The diurnal pattern of this factor shows roughly stable concentrations from 00:00–06:00 LT, which is similar to the aromatic SOA factor. All other factors show a decrease during these hours. It increases by a factor of ∼3 between 11:00–14:00 LT and then steadily decays before being enhanced again by a factor of ∼15 between 18:00–21:00 LT. The daytime increase suggests photochemical production of this factor. The diurnal trend of this factor is stable during late night hours and does not show a marked early morning rush hour peak, indicating little or no influence of morning rush hour emissions.
3.3 Estimation of mass contributions of EESI SOA factors
The EESI-TOF sensitivity towards individual compounds has been shown to vary by up to 1–2 orders of magnitude. Although EESI-TOF factor sensitivities likely vary by significantly less due to averaging effects, these variations nonetheless make it challenging to ascertain relative contributions of EESI-TOF factors on a mass concentration basis. To estimate the EESI-TOF sensitivities (in cps µg−1 m3, where cps denotes counts per second) to different EESI SOA factors and thus obtain a mass-based source apportionment of the resolved SOA factors, a multiple linear regression (MLR) analysis was performed to explain the AMS SOA (i.e. MO-OOA + LO-OOA) time series as a function of the four EESI-TOF SOA factors. Eq. (11) was solved for α1, α2, α3, and α4 where the reciprocal of the coefficients αi represents the sensitivity of the EESI-TOF to each factor in cps µg−1 m3.
To solve Eq. (11), a weighted least-squares approach was used where the uncertainty-weighted residuals (denoted ∈) were minimized for each point in time. The α coefficients for all EESI-TOF SOA factors were constrained such that the obtained sensitivities of these factors were between 0.1 and 1 times that of levoglucosan (∼55 cps µg−1 m3), consistent with previous observations of bulk EESI-TOF sensitivities to SOA from different precursors (Lopez-Hilfiker et al., 2019). In addition to the MLR, the EESI sensitivities towards individual oxidation products were estimated using a gradient-boosting regression–prediction (GBRP) model (Wang et al., 2021) based on their elemental formulae (i.e. CxHyOz). The EESI-TOF sensitivity to different SOA factors was derived by calculating the signal-weighted average based on the factor profile of these individual ion sensitivities. The GBRP model results were used in relative terms, where the response factors obtained for each EESI-TOF factor using the GBRP model were normalized relative to that of primary biomass burning. The EESI-TOF response factor for biomass burning was calculated by taking the ratio of the summed EESI signal in primary biomass burning to the summed AMS BBOA factors. This was then used to scale the sensitivities of the SOA factors obtained using the GBRP model.
The MLR analysis was first applied to the entire time series, which resulted in a correlation coefficient (r) value of 0.6 between modelled SOA (α1× aromatic SOA biogenic SOA aged biomass burning mixed urban SOA) and measured SOA (sum of MO-OOA and LO-OOA from AMS). There were, however, two issues with this analysis. One was that it showed systematic positive and negative biases in certain parts of the time series, and the second was that the fitted MLR coefficients for biogenic SOA, aged biomass burning, and mixed urban SOA were near zero, which, based on previous studies, implied a non-physical result (Lopez-Hilfiker et al., 2019). The possible reason for these mentioned issues might be the presence of a unique event from 18:00 LT on 3 January 2019 to 12:00 LT on 4 January 2019 when high signals of aromatic SOA with low signals of biomass burning and other primary and secondary species were observed, driving the coefficients of all other SOA factors except aromatic SOA to be near zero. Based on the issues mentioned above, the time series was divided into two parts: part 1 from 31 December 2018–3 January 2019 (till 18:00 LT) and part 2 from 4 January 2019 (from 12:00 LT)–13 January 2019. The data from 16:00 LT on 3 January 2019 to 12:00 LT on 4 January 2019 were omitted.
The sensitivities were then obtained by MLR analyses of different parts of the dataset: (1) the sensitivity was estimated by performing MLR on the entire EESI-TOF factor time series; (2) the sensitivity was estimated by performing MLR on only part 1 of the time series; (3) the sensitivity was estimated by performing MLR on only part 2 of the time series; (4) the EESI-TOF sensitivity was assumed to be uniform for all factors, where the bulk EESI sensitivity was calculated as the slope of the total EESI-TOF signal vs. the total AMS organic mass. In addition, the EESI-TOF sensitivity towards individual oxidation products was estimated using a gradient-boosting regression–prediction (GBRP) model (Wang et al., 2021) based on their elemental formulae (i.e. CxHyO) as described above.
The sensitivities obtained using MLR analysis and predicted by the GBRP model were used to calculate modelled SOA, and results were evaluated based on three parameters (Fig. S4): (1) the Pearson correlation coefficient r between the modelled and measured SOA; (2) the mean of the fractional residuals, i.e. measured SOA − modelled SOA measured SOA; and (3) the mean of the scaled residuals, i.e. measured SOA − modelled SOA uncertainty in measured SOA.
The fractional and scaled residuals were closest to zero and hence had the least bias when modelled SOA was calculated by using α coefficients obtained by MLR analysis on part 2 of the time series (Fig. S4). Hence the α coefficients obtained using MLR analysis on part 2 of the time series were applied to the entire time-series factors to calculate a mass-based estimation of the SOA factors. The coefficients obtained were 0.15, 0.11, 0.10, and 0.12 for aromatic SOA, biogenic SOA, aged biomass burning, and mixed urban SOA, respectively. These coefficients correspond to sensitivities of 6.6, 9.1, 10.0, and 8.3 cps µg−1 m3, respectively. As a comparison, the sensitivities predicted by Wang et al. (2021) were 6.1, 8.1, 8.6, and 11.1 cps µg−1 m3 for aromatic SOA, biogenic SOA, aged biomass burning, and mixed urban SOA, respectively, and lay between ± 35 % of those obtained from MLR analysis, providing evidence of robustness of this MLR analysis. Figure S5 shows the time series of measured and modelled SOA obtained using the coefficients derived from the five different strategies discussed above.
3.4 Source apportionment of total OA
Here, we combine MLR-corrected EESI-TOF concentrations for aromatic SOA, biogenic SOA, aged biomass burning, and mixed urban SOA (the sum of which by definition approximates the total AMS-derived SOA) with the AMS source apportionment results for POA factors (i.e. HOA and BBOA) to provide an overall description of the OA sources influencing Delhi. The 24 h average, daytime average (10:00–16:00 LT), and nighttime average (22:00–04:00 LT) factor contributions to total OA mass are shown in Fig. 4. While SOA contributes only 40.0 % of total OA on a daily average basis, there is a stark difference between day and night. SOA constitutes 76.8 % of total OA during the daytime (10:00 to 16:00 LT). The aromatic SOA is the largest contributor to daytime SOA and contributes 55.2 % of SOA during the daytime (42.4 % of total OA), followed by biogenic SOA, which contributes 18.4 % to daytime SOA (14.2 % to total OA). The contributions of aged biomass burning and mixed urban SOA to total SOA during daytime are 11.7 % and 8.5 %, respectively (15.2 % and 11.0 % to total OA). During the nighttime (21:00 to 04:00 LT), SOA constitutes 31.0 % of total OA mass, with biogenic SOA contributing 36.1 % of SOA (11.2 % of total OA) followed by a 25.4 % contribution by aromatic SOA (7.9 % to total OA). Aged biomass burning and mixed urban SOA contribute 15.4 % and 22.9 % to total nighttime SOA, respectively (4.8 % and 7.1 % contribution to total OA, respectively). During the nighttime, the high OA concentrations are driven by high primary emissions into a shallow boundary layer; during the daytime, the OA is dominated by secondary aerosol, including local oxidation in the elevated boundary layer.
The differing relative contributions of primary vs. secondary OA as a function of the time of day have implications for public health policy. Specifically, although POA dominates the overall OA concentration, the SOA factors are most prevalent during times when people are most likely to be outdoors and thus exposed to OA (i.e. daylight). It has been recently shown that oxygenated OA contributes a substantially higher fraction of particle-bound reactive oxygen species (ROS) (Zhou et al., 2019) as compared to primary OA. More specifically, anthropogenic SOA has been shown to be more relevant in terms of oxidative potential (OP) than biogenic SOA and POA (Daellenbach et al., 2020). In a recent study at the same site in Delhi, the ratio of hourly averaged ambient DTT (dithiothreitol) activity in PM2.5 to the NR-PM1 mass concentration (i.e. the intrinsic oxidative potential (OPin)) was found to be highest during the afternoon period (Puthussery et al., 2020). This coincides with the increased contributions from photochemically formed secondary organic aerosol (SOA) as observed in this study. Furthermore, the ratio of anthropogenic to biogenic SOA in Delhi especially during the daytime is high and the SOA fraction is dominated by aromatic SOA. This suggests that the daytime increase in OPin observed by Puthussery et al. (2020) is most likely driven by large contributions from aromatic SOA, which is similar to observations across Europe by Daellenbach et al. (2020). The aromatic SOA is most likely formed from the oxidation of light aromatics emitted by traffic. Reducing traffic emissions, e.g. by cleaning exhaust emissions with catalytic converters, can reduce emission factors of aromatic compounds and may lead to a decrease in total SOA concentration and the oxidative potential of OA.
3.5 Fraction of EESI-TOF factors attributable to local production or emissions during daytime
As discussed previously, the temporal trends of the different factors are likely driven by photochemical production (SOA), emissions (POA), boundary layer dynamics, and gas–particle partitioning. Figure 5 shows the estimated fraction of daytime concentrations attributable to photochemical production for the EESI-TOF SOA factors or direct emissions for EESI-TOF POA factors. AMS-derived PMF factors were not included in this analysis due to the lack of reliable methods to compute saturation vapour concentrations of these factors. The SOA factors (aromatic SOA, aged biomass burning, and mixed urban SOA) have a high mean fraction of daytime photochemical production values of 0.88, 0.82, and 0.83, respectively. This is significantly higher than the daytime photochemical fraction of 0.55 for biogenic SOA (t test, p<0.05). This daytime production suggests that local photochemistry is an important driver for daytime air quality in Delhi and thus relevant to human exposure and health outcomes. As shown in a VOC source apportionment study at the same site (Wang et al., 2020), the largest contributor of primary VOCs during the daytime at this site is a traffic-related factor. This is consistent with high concentrations of light aromatics, which are in turn consistent with the elevated concentration and strong local production term of the EESI-TOF aromatic SOA factor.
The smaller daytime production fraction retrieved for biogenic SOA is consistent with its description as a regionally influenced factor. This is consistent with a projected source distribution that is diffused over a wide area rather than limited to Delhi.
For the primary factors, a relatively small fraction, i.e. 0.53, of primary biomass burning could be attributed to daytime emissions, whereas a relatively high daytime emission fraction, i.e. 0.83, was observed for cooking-related OA, consistent with expectations as primary biomass burning most likely corresponds to nighttime heating activities, while the cooking-related emissions emerge from active sources during specific mealtimes.
Wintertime particulate air pollution in Delhi, India, is a critical public health issue that affects millions of people. Previous studies have identified key POA sources contributing to this pollution and suggested an important role of total SOA. Here we investigate the sources contributing to SOA via source apportionment of the first EESI-TOF deployment in India, in conjunction with AMS source apportionment.
The AMS source apportionment yielded POA factors related to traffic, primary biomass burning (two factors), and SOA (two factors), which in total comprised 60 % and 40 % of the OA mass, respectively. The source apportionment of the EESI-TOF dataset yielded six factors. Two primary factors were identified as primary biomass burning and cooking-related OA, while the remaining four factors were attributed to secondary sources: aromatic SOA, produced from the oxidation of light aromatics emitted by traffic; biogenic SOA, influenced by isoprene and monoterpene oxidation products and of regional influence; aged biomass burning; and mixed urban SOA, containing oxidation products consistent with a mix of sources and processes typical of the Delhi area. Multiple linear regression (MLR) analysis allowed us to calculate response factors for the EESI-TOF SOA factors and enabled apportioning the contribution of each EESI-TOF SOA factor to total SOA mass. During the daytime, SOA dominated, comprising 76.8 % of the total OA mass with 42.4 % contribution from aromatic SOA. The nighttime concentrations were dominated by POA, making up 69.0 % of total OA mass. Large variations in the relative contribution of SOA vs. POA to total OA were observed between the day and night, with anthropogenic SOA sources being major contributors to daytime SOA, explaining the previously observed daytime increase in OP of PM at the same site (Puthussery et al., 2020).
A simple partition-and-dilution modelling analysis was used to estimate the fraction of daytime concentrations that could be attributed to photochemical production for the SOA factors and emissions for the POA factors. Aromatic SOA was found to have the highest photochemical production among all SOA factors, consistent with the high abundance of aromatic VOCs at the site as was previously seen (Wang et al., 2020). Biogenic SOA had significantly lower daytime photochemical production than other SOA factors, indicating its regional nature and that its temporal behaviour is controlled by dilution and partitioning and to a lesser extent by photochemical production. This study reveals that the HOA and BBOA are the main POA sources in Delhi and that aromatic SOA, biogenic SOA, aged biomass burning, and mixed urban SOA constitute total SOA. The daytime OA mass is dominated by SOA, which is mainly composed of aromatic SOA, whereas the nighttime OA is dominated by POA sources of which biomass burning is the dominant one.
The data presented in figures are available in the Zenodo online repository https://doi.org/10.5281/zenodo.6584570 (Kumar, 2022).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-22-7739-2022-supplement.
ASHP, JGS, and SNT designed the study and acquired the necessary funding. VK led the field campaign, carried out formal data analysis, and wrote the manuscript. JGS and VK interpreted the data together. JGS, SG, SLH, YT, CPL, SM, RS, PV, JVP, and DG provided necessary support during the campaign. AS, JSD, and NR provided AMS data. DSW provided GBRP model results. GS, VP, AB, RC, PR, DB, and LQ participated in the campaign from the PSI side. DMB, VV, CM, SNT, ASHP, and UB participated in the interpretation of data. All authors read and edited the manuscript.
The contact author has declared that neither they nor their co-authors have any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Sachchida N. Tripathi gratefully acknowledges the financial support provided by the Department of Biotechnology (DBT), government of India, and the Central Pollution Control Board (CPCB), government of India. Sophie L. Haslett and Claudia Mohr gratefully acknowledge the financial support provided by the Knut and Alice Wallenberg Foundation.
This research has been supported by the SDC Clean Air Project in India (grant no. 7F-10093.01.04); the Swiss National Science Foundation projects BSSGI0_155846 (IPR-80 SHOP), 200021_169787 (SAOPSOAG), and IZLCZ2_169986; the European Union’s Horizon 2020 research and innovation programme under the Marie Skłodowska-Curie Actions (grant no. 701647); and the Knut and Alice Wallenberg Foundation (WAF project CLOUDFORM (grant no. 2017.0165)). Sachchida N. Tripathi was also supported by the Department of Biotechnology (DBT), government of India (grant no. 644), BT/IN/UK/APHH/41/KB/2016-17 dated 19 July 2017, and the Central Pollution Control Board (CPCB), government of India, under grant no. AQM/Source apportionment_EPC Project/2017.
This paper was edited by Tuukka Petäjä and reviewed by two anonymous referees.
Aiken, A. C., Salcedo, D., Cubison, M. J., Huffman, J. A., DeCarlo, P. F., Ulbrich, I. M., Docherty, K. S., Sueper, D., Kimmel, J. R., Worsnop, D. R., Trimborn, A., Northway, M., Stone, E. A., Schauer, J. J., Volkamer, R. M., Fortner, E., de Foy, B., Wang, J., Laskin, A., Shutthanandan, V., Zheng, J., Zhang, R., Gaffney, J., Marley, N. A., Paredes-Miranda, G., Arnott, W. P., Molina, L. T., Sosa, G., and Jimenez, J. L.: Mexico City aerosol analysis during MILAGRO using high resolution aerosol mass spectrometry at the urban supersite (T0) – Part 1: Fine particle composition and organic source apportionment, Atmos. Chem. Phys., 9, 6633–6653, https://doi.org/10.5194/acp-9-6633-2009, 2009.
Allan, J. D., Jimenez, J. L., Williams, P. I., Alfarra, M. R., Bower, K. N., Jayne, J. T., Coe, H., and Worsnop, D. R.: Quantitative sampling using an Aerodyne aerosol mass spectrometer 1. Techniques of data interpretation and error analysis, J. Geophys. Res.-Atmos., 108, 4090, https://doi.org/10.1029/2002JD002358, 2003.
Bertrand, A., Stefenelli, G., Jen, C. N., Pieber, S. M., Bruns, E. A., Ni, H., Temime-Roussel, B., Slowik, J. G., Goldstein, A. H., El Haddad, I., Baltensperger, U., Prévôt, A. S. H., Wortham, H., and Marchand, N.: Evolution of the chemical fingerprint of biomass burning organic aerosol during aging, Atmos. Chem. Phys., 18, 7607–7624, https://doi.org/10.5194/acp-18-7607-2018, 2018.
Bhandari, S., Gani, S., Patel, K., Wang, D. S., Soni, P., Arub, Z., Habib, G., Apte, J. S., and Hildebrandt Ruiz, L.: Sources and atmospheric dynamics of organic aerosol in New Delhi, India: insights from receptor modeling, Atmos. Chem. Phys., 20, 735–752, https://doi.org/10.5194/acp-20-735-2020, 2020.
Bruns, E. A., Krapf, M., Orasche, J., Huang, Y., Zimmermann, R., Drinovec, L., Močnik, G., El-Haddad, I., Slowik, J. G., Dommen, J., Baltensperger, U., and Prévôt, A. S. H.: Characterization of primary and secondary wood combustion products generated under different burner loads, Atmos. Chem. Phys., 15, 2825–2841, https://doi.org/10.5194/acp-15-2825-2015, 2015.
Canagaratna, M. R., Jayne, J. T., Jimenez, J. L., Allan, J. D., Alfarra, M. R., Zhang, Q., Onasch, T. B., Drewnick, F., Coe, H., Middlebrook, A., Delia, A., Williams, L. R., Trimborn, A. M., Northway, M. J., DeCarlo, P. F., Kolb, C. E., Davidovits, P., and Worsnop, D. R.: Chemical and microphysical characterization of ambient aerosols with the aerodyne aerosol mass spectrometer, Mass Spectrom. Rev., 26, 185–222, https://doi.org/10.1002/mas.20115, 2007.
Canonaco, F., Crippa, M., Slowik, J. G., Baltensperger, U., and Prévôt, A. S. H.: SoFi, an IGOR-based interface for the efficient use of the generalized multilinear engine (ME-2) for the source apportionment: ME-2 application to aerosol mass spectrometer data, Atmos. Meas. Tech., 6, 3649–3661, https://doi.org/10.5194/amt-6-3649-2013, 2013.
Cao, X., Yao, Z., Shen, X., Ye, Y., and Jiang, X.: On-road emission characteristics of VOCs from light-duty gasoline vehicles in Beijing, China, Atmos. Environ., 124, 146–155, https://doi.org/10.1016/j.atmosenv.2015.06.019, 2016.
Central Pollution Control Board: National ambient air quality standards (NAAQs), https://cpcb.nic.in/uploads/National_Ambient_Air_Quality_Standards.pdf (last access: 10 November 2021), 2009.
Chen, Y., Takeuchi, M., Nah, T., Xu, L., Canagaratna, M. R., Stark, H., Baumann, K., Canonaco, F., Prévôt, A. S. H., Huey, L. G., Weber, R. J., and Ng, N. L.: Chemical characterization of secondary organic aerosol at a rural site in the southeastern US: insights from simultaneous high-resolution time-of-flight aerosol mass spectrometer (HR-ToF-AMS) and FIGAERO chemical ionization mass spectrometer (CIMS) measurements, Atmos. Chem. Phys., 20, 8421–8440, https://doi.org/10.5194/acp-20-8421-2020, 2020.
Crippa, M., DeCarlo, P. F., Slowik, J. G., Mohr, C., Heringa, M. F., Chirico, R., Poulain, L., Freutel, F., Sciare, J., Cozic, J., Di Marco, C. F., Elsasser, M., Nicolas, J. B., Marchand, N., Abidi, E., Wiedensohler, A., Drewnick, F., Schneider, J., Borrmann, S., Nemitz, E., Zimmermann, R., Jaffrezo, J.-L., Prévôt, A. S. H., and Baltensperger, U.: Wintertime aerosol chemical composition and source apportionment of the organic fraction in the metropolitan area of Paris, Atmos. Chem. Phys., 13, 961–981, https://doi.org/10.5194/acp-13-961-2013, 2013.
Crippa, M., Canonaco, F., Lanz, V. A., Äijälä, M., Allan, J. D., Carbone, S., Capes, G., Ceburnis, D., Dall'Osto, M., Day, D. A., DeCarlo, P. F., Ehn, M., Eriksson, A., Freney, E., Hildebrandt Ruiz, L., Hillamo, R., Jimenez, J. L., Junninen, H., Kiendler-Scharr, A., Kortelainen, A.-M., Kulmala, M., Laaksonen, A., Mensah, A. A., Mohr, C., Nemitz, E., O'Dowd, C., Ovadnevaite, J., Pandis, S. N., Petäjä, T., Poulain, L., Saarikoski, S., Sellegri, K., Swietlicki, E., Tiitta, P., Worsnop, D. R., Baltensperger, U., and Prévôt, A. S. H.: Organic aerosol components derived from 25 AMS data sets across Europe using a consistent ME-2 based source apportionment approach, Atmos. Chem. Phys., 14, 6159–6176, https://doi.org/10.5194/acp-14-6159-2014, 2014.
Daellenbach, K. R., Uzu, G., Jiang, J., Cassagnes, L.-E., Leni, Z., Vlachou, A., Stefenelli, G., Canonaco, F., Weber, S., Segers, A., Kuenen, J. J. P., Schaap, M., Favez, O., Albinet, A., Aksoyoglu, S., Dommen, J., Baltensperger, U., Geiser, M., El Haddad, I., Jaffrezo, J.-L., and Prévôt, A. S. H.: Sources of particulate-matter air pollution and its oxidative potential in Europe, Nature, 587, 414–419, https://doi.org/10.1038/s41586-020-2902-8, 2020.
Davison, A. C. and Hinkley, D. V.: Bootstrap Methods and Their Application, Cambridge University Press, https://doi.org/10.1017/CBO9780511802843, 1997.
DeCarlo, P. F., Kimmel, J. R., Trimborn, A., Northway, M. J., Jayne, J. T., Aiken, A. C., Gonin, M., Fuhrer, K., Horvath, T., Docherty, K. S., Worsnop, D. R., and Jimenez, J. L.: Field-Deployable, High-Resolution, Time-of-Flight Aerosol Mass Spectrometer, Anal. Chem., 78, 8281–8289, https://doi.org/10.1021/ac061249n, 2006.
Donahue, N. M., Robinson, A. L., Stanier, C. O., and Pandis, S. N.: Coupled Partitioning, Dilution, and Chemical Aging of Semivolatile Organics, Environ. Sci. Technol., 40, 2635–2643, https://doi.org/10.1021/es052297c, 2006.
Donahue, N. M., Epstein, S. A., Pandis, S. N., and Robinson, A. L.: A two-dimensional volatility basis set: 1. organic-aerosol mixing thermodynamics, Atmos. Chem. Phys., 11, 3303–3318, https://doi.org/10.5194/acp-11-3303-2011, 2011.
Duplissy, J., DeCarlo, P. F., Dommen, J., Alfarra, M. R., Metzger, A., Barmpadimos, I., Prevot, A. S. H., Weingartner, E., Tritscher, T., Gysel, M., Aiken, A. C., Jimenez, J. L., Canagaratna, M. R., Worsnop, D. R., Collins, D. R., Tomlinson, J., and Baltensperger, U.: Relating hygroscopicity and composition of organic aerosol particulate matter, Atmos. Chem. Phys., 11, 1155–1165, https://doi.org/10.5194/acp-11-1155-2011, 2011.
Dzepina, K., Arey, J., Marr, L. C., Worsnop, D. R., Salcedo, D., Zhang, Q., Onasch, T. B., Molina, L. T., Molina, M. J., and Jimenez, J. L.: Detection of particle-phase polycyclic aromatic hydrocarbons in Mexico City using an aerosol mass spectrometer, Int. J. Mass Spectrom., 263, 152–170, https://doi.org/10.1016/j.ijms.2007.01.010, 2007.
Eichler, P., Müller, M., D'Anna, B., and Wisthaler, A.: A novel inlet system for online chemical analysis of semi-volatile submicron particulate matter, Atmos. Meas. Tech., 8, 1353–1360, https://doi.org/10.5194/amt-8-1353-2015, 2015.
Forster, P., Ramaswamy, V., Artaxo, P., Berntsen, T., Betts, R., Fahey, D. W., Haywood, J., Lean, J., Lowe, D. C., Myhre, G., Nganga, J., Prinn, R., Raga, G., Schulz, M., and Van Dorland, R.: Changes in Atmospheric Constituents and in Radiative Forcing, in: Climate Change 2007: The Physical Science Basis. Contribution of Working Group I to the Fourth Assessment Report of the Intergovernmental Panel on Climate Change, edited by: Solomon, S., Qin, D., Manning, M., Chen, Z., Marquis, M., Averyt, K. B., Tignor, M., and Miller, H. L., Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, 2007.
Gani, S., Bhandari, S., Seraj, S., Wang, D. S., Patel, K., Soni, P., Arub, Z., Habib, G., Hildebrandt Ruiz, L., and Apte, J. S.: Submicron aerosol composition in the world's most polluted megacity: the Delhi Aerosol Supersite study, Atmos. Chem. Phys., 19, 6843–6859, https://doi.org/10.5194/acp-19-6843-2019, 2019.
Guenther, A. B., Jiang, X., Heald, C. L., Sakulyanontvittaya, T., Duhl, T., Emmons, L. K., and Wang, X.: The Model of Emissions of Gases and Aerosols from Nature version 2.1 (MEGAN2.1): an extended and updated framework for modeling biogenic emissions, Geosci. Model Dev., 5, 1471–1492, https://doi.org/10.5194/gmd-5-1471-2012, 2012.
Hallquist, M., Wenger, J. C., Baltensperger, U., Rudich, Y., Simpson, D., Claeys, M., Dommen, J., Donahue, N. M., George, C., Goldstein, A. H., Hamilton, J. F., Herrmann, H., Hoffmann, T., Iinuma, Y., Jang, M., Jenkin, M. E., Jimenez, J. L., Kiendler-Scharr, A., Maenhaut, W., McFiggans, G., Mentel, Th. F., Monod, A., Prévôt, A. S. H., Seinfeld, J. H., Surratt, J. D., Szmigielski, R., and Wildt, J.: The formation, properties and impact of secondary organic aerosol: current and emerging issues, Atmos. Chem. Phys., 9, 5155–5236, https://doi.org/10.5194/acp-9-5155-2009, 2009.
Haslett, S. L., Bell, D. M., Kumar, V., Slowik, J. G., Mishra, S., Rastogi, N., Singh, A., Ganguly, D., Thornton, J., Dällenbach, K., Yan, C., Kulmala, M., Liu, Y., Zheng, F., Nie, W., Li, Y., Tripathi, S. N., and Mohr, C.: Night-time NO emissions suppress large amounts of chlorine radical formation in Delhi, Science Advances, submitted, 2022.
Hoffmann, D., Tilgner, A., Iinuma, Y., and Herrmann, H.: Atmospheric stability of levoglucosan: a detailed laboratory and modeling study, Environ. Sci. Technol., 44, 694–699, 2010.
Jimenez, J. L., Jayne, J. T., Shi, Q., Kolb, C. E., Worsnop, D. R., Yourshaw, I., Seinfeld, J. H., Flagan, R. C., Zhang, X., Smith, K. A., Morris, J. W., and Davidovits, P.: Ambient aerosol sampling using the Aerodyne Aerosol Mass Spectrometer, J. Geophys. Res.-Atmos., 108, 8425, https://doi.org/10.1029/2001JD001213, 2003.
Jimenez, J. L., Canagaratna, M. R., Donahue, N. M., Prevot, A. S. H., Zhang, Q., Kroll, J. H., DeCarlo, P. F., Allan, J. D., Coe, H., Ng, N. L., Aiken, A. C., Docherty, K. S., Ulbrich, I. M., Grieshop, A. P., Robinson, A. L., Duplissy, J., Smith, J. D., Wil-son, K. R., Lanz, V. A., Hueglin, C., Sun, Y. L., Tian, J., Laaksonen, A., Raatikainen, T., Rautiainen, J., Vaattovaara, P., Ehn, M., Kulmala, M., Tomlinson, J. M., Collins, D. R., Cubison, M. J., Dunlea, J., Huffman, J. A., Onasch, T. B., Alfarra, M. R., Williams, P. I., Bower, K., Kondo, Y., Schneider, J., Drewnick, F., Borrmann, S., Weimer, S., Demerjian, K., Salcedo, D., Cottrell, L., Griffin, R., Takami, A., Miyoshi, T., Hatakeyama, S., Shimono, A., Sun, J. Y., Zhang, Y. M., Dzepina, K., Kimmel, J. R., Sueper, D., Jayne, J. T., Herndon, S. C., Trimborn, A. M., Williams, L. R., Wood, E. C., Middlebrook, A. M., Kolb, C. E., Baltensperger, U., and Worsnop, D. R.: Evolution of Organic Aerosols in the Atmosphere, Science, 326, 1525–1529, https://doi.org/10.1126/science.1180353, 2009.
Kristensen, K., Bilde, M., Aalto, P. P., Petäjä, T., and Glasius, M.: Denuder/filter sampling of organic acids and organosulfates at urban and boreal forest sites: Gas/particle distribution and possible sampling artifacts, Atmos. Environ., 130, 36–53, https://doi.org/10.1016/j.atmosenv.2015.10.046, 2016.
Kumar, V.: Highly time-resolved chemical speciation and source apportionment of organic aerosol components in Delhi, India, using extractive electrospray ionization mass spectrometry, Zenodo[Data set], https://doi.org/10.5281/zenodo.6584570, 2022.
Kumar, V., Slowik, J. G., Baltensperger, U., Prevot, A. S. H., and Bell, D. M.: Particle phase composition and evolution of secondary organic aerosol (SOA) formed from oxidation of a mixture of aromatics by OH and NO3 radicals, in preparation, 2022.
Lalchandani, V., Kumar, V., Tobler, A., M. Thamban, N., Mishra, S., Slowik, J. G., Bhattu, D., Rai, P., Satish, R., Ganguly, D., Tiwari, S., Rastogi, N., Tiwari, S., Močnik, G., Prévôt, A. S. H., and Tripathi, S. N.: Real-time characterization and source apportionment of fine particulate matter in the Delhi megacity area during late winter, Sci. Total Environ., 770, 145324, https://doi.org/10.1016/j.scitotenv.2021.145324, 2021.
Lanz, V. A., Alfarra, M. R., Baltensperger, U., Buchmann, B., Hueglin, C., and Prévôt, A. S. H.: Source apportionment of submicron organic aerosols at an urban site by factor analytical modelling of aerosol mass spectra, Atmos. Chem. Phys., 7, 1503–1522, https://doi.org/10.5194/acp-7-1503-2007, 2007.
Li, Y., Pöschl, U., and Shiraiwa, M.: Molecular corridors and parameterizations of volatility in the chemical evolution of organic aerosols, Atmos. Chem. Phys., 16, 3327–3344, https://doi.org/10.5194/acp-16-3327-2016, 2016.
Lopez-Hilfiker, F. D., Mohr, C., Ehn, M., Rubach, F., Kleist, E., Wildt, J., Mentel, Th. F., Lutz, A., Hallquist, M., Worsnop, D., and Thornton, J. A.: A novel method for online analysis of gas and particle composition: description and evaluation of a Filter Inlet for Gases and AEROsols (FIGAERO), Atmos. Meas. Tech., 7, 983–1001, https://doi.org/10.5194/amt-7-983-2014, 2014.
Lopez-Hilfiker, F. D., Pospisilova, V., Huang, W., Kalberer, M., Mohr, C., Stefenelli, G., Thornton, J. A., Baltensperger, U., Prevot, A. S. H., and Slowik, J. G.: An extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF) for online measurement of atmospheric aerosol particles, Atmos. Meas. Tech., 12, 4867–4886, https://doi.org/10.5194/amt-12-4867-2019, 2019.
Mehra, A., Wang, Y., Krechmer, J. E., Lambe, A., Majluf, F., Morris, M. A., Priestley, M., Bannan, T. J., Bryant, D. J., Pereira, K. L., Hamilton, J. F., Rickard, A. R., Newland, M. J., Stark, H., Croteau, P., Jayne, J. T., Worsnop, D. R., Canagaratna, M. R., Wang, L., and Coe, H.: Evaluation of the chemical composition of gas- and particle-phase products of aromatic oxidation, Atmos. Chem. Phys., 20, 9783–9803, https://doi.org/10.5194/acp-20-9783-2020, 2020.
Middlebrook, A. M., Bahreini, R., Jimenez, J. L., and Canagaratna, M. R.: Evaluation of Composition-Dependent Collection Efficiencies for the Aerodyne Aerosol Mass Spectrometer using Field Data, Aerosol Sci. Technol., 46, 258–271, https://doi.org/10.1080/02786826.2011.620041, 2012.
Mohr, C., Thornton, J. A., Heitto, A., Lopez-Hilfiker, F. D., Lutz, A., Riipinen, I., Hong, J., Donahue, N. M., Hallquist, M., Petäjä, T., Kulmala, M., and Yli-Juuti, T.: Molecular identification of organic vapors driving atmospheric nanoparticle growth, Nat. Commun., 10, 4442, https://doi.org/10.1038/s41467-019-12473-2, 2019.
Müller, M., Eichler, P., D'Anna, B., Tan, W., and Wisthaler, A.: Direct Sampling and Analysis of Atmospheric Particulate Organic Matter by Proton-Transfer-Reaction Mass Spectrometry, Anal. Chem., 89, 10889–10897, https://doi.org/10.1021/acs.analchem.7b02582, 2017.
Ng, N. L., Canagaratna, M. R., Zhang, Q., Jimenez, J. L., Tian, J., Ulbrich, I. M., Kroll, J. H., Docherty, K. S., Chhabra, P. S., Bahreini, R., Murphy, S. M., Seinfeld, J. H., Hildebrandt, L., Donahue, N. M., DeCarlo, P. F., Lanz, V. A., Prévôt, A. S. H., Dinar, E., Rudich, Y., and Worsnop, D. R.: Organic aerosol components observed in Northern Hemispheric datasets from Aerosol Mass Spectrometry, Atmos. Chem. Phys., 10, 4625–4641, https://doi.org/10.5194/acp-10-4625-2010, 2010.
Orsavova, J., Misurcova, L., Ambrozova, J. V., Vicha, R., and Mlcek, J.: Fatty Acids Composition of Vegetable Oils and Its Contribution to Dietary Energy Intake and Dependence of Cardiovascular Mortality on Dietary Intake of Fatty Acids, Int. J. Mol. Sci., 16, 12871–12890, https://doi.org/10.3390/ijms160612871, 2015.
Paatero, P.: The Multilinear Engine – A Table-Driven, Least Squares Program for Solving Multilinear Problems, Including the n-Way Parallel Factor Analysis Model, J. Comput. Graph. Stat., 8, 854–888, https://doi.org/10.1080/10618600.1999.10474853, 1999.
Paatero, P. and Hopke, P. K.: Discarding or downweighting high-noise variables in factor analytic models, Anal. Chim. Acta, 490, 277–289, https://doi.org/10.1016/S0003-2670(02)01643-4, 2003.
Paatero, P. and Tapper, U.: Positive matrix factorization: A non-negative factor model with optimal utilization of error estimates of data values, Environmetrics, 5, 111–126, https://doi.org/10.1002/env.3170050203, 1994.
Paatero, P., Eberly, S., Brown, S. G., and Norris, G. A.: Methods for estimating uncertainty in factor analytic solutions, Atmos. Meas. Tech., 7, 781–797, https://doi.org/10.5194/amt-7-781-2014, 2014.
Pankow, J. F. and Asher, W. E.: SIMPOL.1: a simple group contribution method for predicting vapor pressures and enthalpies of vaporization of multifunctional organic compounds, Atmos. Chem. Phys., 8, 2773–2796, https://doi.org/10.5194/acp-8-2773-2008, 2008.
Pieber, S. M., El Haddad, I., Slowik, J. G., Canagaratna, M. R., Jayne, J. T., Platt, S. M., Bozzetti, C., Daellenbach, K. R., Fröhlich, R., Vlachou, A., Klein, F., Dommen, J., Miljevic, B., Jiménez, J. L., Worsnop, D. R., Baltensperger, U., and Prévôt, A. S. H.: Inorganic Salt Interference on in Aerodyne AMS and ACSM Organic Aerosol Composition Studies, Environ. Sci. Technol., 50, 10494–10503, https://doi.org/10.1021/acs.est.6b01035, 2016.
Planning Department; Government of NCT of Delhi: Economic Survey of Delhi, http://delhiplanning.nic.in/sites/default/files/E19_Demography.pdf (last access: 11 May 2022), 2021.
Platt, S. M., El Haddad, I., Pieber, S. M., Zardini, A. A., Suarez-Bertoa, R., Clairotte, M., Daellenbach, K. R., Huang, R.-J., Slowik, J. G., Hellebust, S., Temime-Roussel, B., Marchand, N., de Gouw, J., Jimenez, J. L., Hayes, P. L., Robinson, A. L., Baltensperger, U., Astorga, C., and Prévôt, A. S. H.: Gasoline cars produce more carbonaceous particulate matter than modern filter-equipped diesel cars, Sci. Rep., 7, 4926, https://doi.org/10.1038/s41598-017-03714-9, 2017.
Pope, C. A., Ezzati, M., and Dockery, D. W.: Fine-Particulate Air Pollution and Life Expectancy in the United States, N. Engl. J. Med., 360, 376–386, https://doi.org/10.1056/NEJMsa0805646, 2009.
Pospisilova, V., Lopez-Hilfiker, F. D., Bell, D. M., El Haddad, I., Mohr, C., Huang, W., Heikkinen, L., Xiao, M., Dommen, J., Prevot, A. S. H., Baltensperger, U., and Slowik, J. G.: On the fate of oxygenated organic molecules in atmospheric aerosol particles, Science Advances, 6, eaax8922, https://doi.org/10.1126/sciadv.aax8922, 2020.
Puthussery, J. V, Singh, A., Rai, P., Bhattu, D., Kumar, V., Vats, P., Furger, M., Rastogi, N., Slowik, J. G., Ganguly, D., Prevot, A. S. H., Tripathi, S. N., and Verma, V.: Real-Time Measurements of PM2.5 Oxidative Potential Using a Dithiothreitol Assay in Delhi, India, Environ. Sci. Technol. Lett., 7, 504–510, https://doi.org/10.1021/acs.estlett.0c00342, 2020.
Qi, L., Chen, M., Stefenelli, G., Pospisilova, V., Tong, Y., Bertrand, A., Hueglin, C., Ge, X., Baltensperger, U., Prévôt, A. S. H., and Slowik, J. G.: Organic aerosol source apportionment in Zurich using an extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF-MS) – Part 2: Biomass burning influences in winter, Atmos. Chem. Phys., 19, 8037–8062, https://doi.org/10.5194/acp-19-8037-2019, 2019.
Qi, L., Vogel, A. L., Esmaeilirad, S., Cao, L., Zheng, J., Jaffrezo, J.-L., Fermo, P., Kasper-Giebl, A., Daellenbach, K. R., Chen, M., Ge, X., Baltensperger, U., Prévôt, A. S. H., and Slowik, J. G.: A 1-year characterization of organic aerosol composition and sources using an extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF), Atmos. Chem. Phys., 20, 7875–7893, https://doi.org/10.5194/acp-20-7875-2020, 2020.
Rai, P., Furger, M., El Haddad, I., Kumar, V., Wang, L., Singh, A., Dixit, K., Bhattu, D., Petit, J.-E., Ganguly, D., Rastogi, N., Baltensperger, U., Tripathi, S. N., Slowik, J. G., and Prévôt, A. S. H.: Real-time measurement and source apportionment of elements in Delhi's atmosphere, Sci. Total Environ., 742, 140332, https://doi.org/10.1016/j.scitotenv.2020.140332, 2020.
Rolph, G., Stein, A., and Stunder, B.: Real-time Environmental Applications and Display sYstem: READY, Environ. Model. Softw., 95, 210–228, https://doi.org/10.1016/j.envsoft.2017.06.025, 2017.
Salvi, S.: Health effects of ambient air pollution in children, Paediatr. Respir. Rev., 8, 275–280, https://doi.org/10.1016/j.prrv.2007.08.008, 2007.
Sembhi, H., Wooster, M., Zhang, T., Sharma, S., Singh, N., Agarwal, S., Boesch, H., Gupta, S., Misra, A., Tripathi, S. N., Mor, S., and Khaiwal, R.: Post-monsoon air quality degradation across Northern India: assessing the impact of policy-related shifts in timing and amount of crop residue burnt, Environ. Res. Lett., 15, 104067, https://doi.org/10.1088/1748-9326/aba714, 2020.
Shiraiwa, M., Ueda, K., Pozzer, A., Lammel, G., Kampf, C. J., Fushimi, A., Enami, S., Arangio, A. M., Fröhlich-Nowoisky, J., Fujitani, Y., Furuyama, A., Lakey, P. S. J., Lelieveld, J., Lucas, K., Morino, Y., Pöschl, U., Takahama, S., Takami, A., Tong, H., Weber, B., Yoshino, A., and Sato, K.: Aerosol Health Effects from Molecular to Global Scales, Environ. Sci. Technol., 51, 13545–13567, https://doi.org/10.1021/acs.est.7b04417, 2017.
Shrivastava, M., Cappa, C. D., Fan, J., Goldstein, A. H., Guenther, A. B., Jimenez, J. L., Kuang, C., Laskin, A., Martin, S. T., Ng, N. L., Petaja, T., Pierce, J. R., Rasch, P. J., Roldin, P., Seinfeld, J. H., Shilling, J., Smith, J. N., Thornton, J. A., Volkamer, R., Wang, J., Worsnop, D. R., Zaveri, R. A., Zelenyuk, A., and Zhang, Q.: Recent advances in understanding secondary organic aerosol: Implications for global climate forcing, Rev. Geophys., 55, 509–559, https://doi.org/10.1002/2016RG000540, 2017.
Simoneit, B. R. T., Schauer, J. J., Nolte, C. G., Oros, D. R., Elias, V. O., Fraser, M. P., Rogge, W. F., and Cass, G. R.: Levoglucosan, a tracer for cellulose in biomass burning and atmospheric particles, Atmos. Environ., 33, 173–182, https://doi.org/10.1016/S1352-2310(98)00145-9, 1999.
Sindelarova, K., Granier, C., Bouarar, I., Guenther, A., Tilmes, S., Stavrakou, T., Müller, J.-F., Kuhn, U., Stefani, P., and Knorr, W.: Global data set of biogenic VOC emissions calculated by the MEGAN model over the last 30 years, Atmos. Chem. Phys., 14, 9317–9341, https://doi.org/10.5194/acp-14-9317-2014, 2014.
Singh, A., Satish, R. V., and Rastogi, N.: Characteristics and sources of fine organic aerosol over a big semi-arid urban city of western India using HR-ToF-AMS, Atmos. Environ., 208, 103–112, https://doi.org/10.1016/j.atmosenv.2019.04.009, 2019.
Singh, A., Rastogi, N., Kumar, V., Slowik, J. G., Satish, R., Lalchandani, V., Thamban, N. M., Rai, P., Bhattu, D., Vats, P., Ganguly, D., Tripathi, S. N., and Prévôt, A. S. H.: Sources and characteristics of light-absorbing fine particulates over Delhi through the synergy of real-time optical and chemical measurements, Atmos. Environ., 252, 118338, https://doi.org/10.1016/j.atmosenv.2021.118338, 2021.
Stark, H., Yatavelli, R. L. N., Thompson, S. L., Kang, H., Krechmer, J. E., Kimmel, J. R., Palm, B. B., Hu, W., Hayes, P. L., Day, D. A., Campuzano-Jost, P., Canagaratna, M. R., Jayne, J. T., Worsnop, D. R., and Jimenez, J. L.: Impact of Thermal Decomposition on Thermal Desorption Instruments: Advantage of Thermogram Analysis for Quantifying Volatility Distributions of Organic Species, Environ. Sci. Technol., 51, 8491–8500, https://doi.org/10.1021/acs.est.7b00160, 2017.
Stefenelli, G., Pospisilova, V., Lopez-Hilfiker, F. D., Daellenbach, K. R., Hüglin, C., Tong, Y., Baltensperger, U., Prévôt, A. S. H., and Slowik, J. G.: Organic aerosol source apportionment in Zurich using an extractive electrospray ionization time-of-flight mass spectrometer (EESI-TOF-MS) – Part 1: Biogenic influences and day–night chemistry in summer, Atmos. Chem. Phys., 19, 14825–14848, https://doi.org/10.5194/acp-19-14825-2019, 2019.
Tobler, A., Bhattu, D., Canonaco, F., Lalchandani, V., Shukla, A., Thamban, N. M., Mishra, S., Srivastava, A. K., Bisht, D. S., Tiwari, S., Singh, S., Močnik, G., Baltensperger, U., Tripathi, S. N., Slowik, J. G., and Prévôt, A. S. H.: Chemical characterization of PM2.5 and source apportionment of organic aerosol in New Delhi, India, Sci. Total Environ., 745, 140924, https://doi.org/10.1016/j.scitotenv.2020.140924, 2020.
Tong, Y., Pospisilova, V., Qi, L., Duan, J., Gu, Y., Kumar, V., Rai, P., Stefenelli, G., Wang, L., Wang, Y., Zhong, H., Baltensperger, U., Cao, J., Huang, R.-J., Prévôt, A. S. H., and Slowik, J. G.: Quantification of solid fuel combustion and aqueous chemistry contributions to secondary organic aerosol during wintertime haze events in Beijing, Atmos. Chem. Phys., 21, 9859–9886, https://doi.org/10.5194/acp-21-9859-2021, 2021.
Tröstl, J., Chuang, W. K., Gordon, H., Heinritzi, M., Yan, C., Molteni, U., Ahlm, L., Frege, C., Bianchi, F., Wagner, R., Simon, M., Lehtipalo, K., Williamson, C., Craven, J. S., Duplissy, J., Adamov, A., Almeida, J., Bernhammer, A. K., Breitenlechner, M., Brilke, S., Dias, A., Ehrhart, S., Flagan, R. C., Franchin, A., Fuchs, C., Guida, R., Gysel, M., Hansel, A., Hoyle, C. R., Jokinen, T., Junninen, H., Kangasluoma, J., Keskinen, H., Kim, J., Krapf, M., Kürten, A., Laaksonen, A., Lawler, M., Leiminger, M., Mathot, S., Möhler, O., Nieminen, T., Onnela, A., Petäjä, T., Piel, F. M., Miettinen, P., Rissanen, M. P., Rondo, L., Sarnela, N., Schobesberger, S., Sengupta, K., Sipilä, M., Smith, J. N., Steiner, G., Tomè, A., Virtanen, A., Wagner, A. C., Weingartner, E., Wimmer, D., Winkler, P. M., Ye, P., Carslaw, K. S., Curtius, J., Dommen, J., Kirkby, J., Kulmala, M., Riipinen, I., Worsnop, D. R., Donahue, N. M., and Baltensperger, U.: The role of low-volatility organic compounds in initial particle growth in the atmosphere, Nature, 533, 527–531, https://doi.org/10.1038/nature18271, 2016.
Ulbrich, I. M., Canagaratna, M. R., Zhang, Q., Worsnop, D. R., and Jimenez, J. L.: Interpretation of organic components from Positive Matrix Factorization of aerosol mass spectrometric data, Atmos. Chem. Phys., 9, 2891–2918, https://doi.org/10.5194/acp-9-2891-2009, 2009.
Wang, D. S., Lee, C. P., Krechmer, J. E., Majluf, F., Tong, Y., Canagaratna, M. R., Schmale, J., Prévôt, A. S. H., Baltensperger, U., Dommen, J., El Haddad, I., Slowik, J. G., and Bell, D. M.: Constraining the response factors of an extractive electrospray ionization mass spectrometer for near-molecular aerosol speciation, Atmos. Meas. Tech., 14, 6955–6972, https://doi.org/10.5194/amt-14-6955-2021, 2021.
Wang, L., Slowik, J. G., Tripathi, N., Bhattu, D., Rai, P., Kumar, V., Vats, P., Satish, R., Baltensperger, U., Ganguly, D., Rastogi, N., Sahu, L. K., Tripathi, S. N., and Prévôt, A. S. H.: Source characterization of volatile organic compounds measured by proton-transfer-reaction time-of-flight mass spectrometers in Delhi, India, Atmos. Chem. Phys., 20, 9753–9770, https://doi.org/10.5194/acp-20-9753-2020, 2020.
Williams, L. R., Gonzalez, L. A., Peck, J., Trimborn, D., McInnis, J., Farrar, M. R., Moore, K. D., Jayne, J. T., Robinson, W. A., Lewis, D. K., Onasch, T. B., Canagaratna, M. R., Trimborn, A., Timko, M. T., Magoon, G., Deng, R., Tang, D., de la Rosa Blanco, E., Prévôt, A. S. H., Smith, K. A., and Worsnop, D. R.: Characterization of an aerodynamic lens for transmitting particles greater than 1 micrometer in diameter into the Aerodyne aerosol mass spectrometer, Atmos. Meas. Tech., 6, 3271–3280, https://doi.org/10.5194/amt-6-3271-2013, 2013.
World Health Organisation: WHO Global Ambient Air Quality Database (update 2018), Ambient Air Quality Database, https://www.who.int/data/gho/data/themes/air-pollution/who-air-quality-database#cms (last access: 7 June 2022), 2018.
Yao, Z., Shen, X., Ye, Y., Cao, X., Jiang, X., Zhang, Y., and He, K.: On-road emission characteristics of VOCs from diesel trucks in Beijing, China, Atmos. Environ., 103, 87–93, https://doi.org/10.1016/j.atmosenv.2014.12.028, 2015.
Yee, L. D., Kautzman, K. E., Loza, C. L., Schilling, K. A., Coggon, M. M., Chhabra, P. S., Chan, M. N., Chan, A. W. H., Hersey, S. P., Crounse, J. D., Wennberg, P. O., Flagan, R. C., and Seinfeld, J. H.: Secondary organic aerosol formation from biomass burning intermediates: phenol and methoxyphenols, Atmos. Chem. Phys., 13, 8019–8043, https://doi.org/10.5194/acp-13-8019-2013, 2013.
Zhang, Q., Jimenez, J. L., Canagaratna, M. R., Ulbrich, I. M., Ng, N. L., Worsnop, D. R., and Sun, Y.: Understanding atmospheric organic aerosols via factor analysis of aerosol mass spectrometry: a review, Anal. Bioanal. Chem., 401, 3045–3067, https://doi.org/10.1007/s00216-011-5355-y, 2011.
Zhang, Y., Wang, X., Barletta, B., Simpson, I. J., Blake, D. R., Fu, X., Zhang, Z., He, Q., Liu, T., Zhao, X., and Ding, X.: Source attributions of hazardous aromatic hydrocarbons in urban, suburban and rural areas in the Pearl River Delta (PRD) region, J. Hazard. Mater., 250–251, 403–411, https://doi.org/10.1016/j.jhazmat.2013.02.023, 2013.
Zhao, R., Kenseth, C. M., Huang, Y., Dalleska, N. F., and Seinfeld, J. H.: Iodometry-assisted liquid chromatography electrospray ionization mass spectrometry for analysis of organic peroxides: An application to atmospheric secondary organic aerosol, Environ. Sci. Technol., 52, 2108–2117, 2018.
Zhou, J., Elser, M., Huang, R.-J., Krapf, M., Fröhlich, R., Bhattu, D., Stefenelli, G., Zotter, P., Bruns, E. A., Pieber, S. M., Ni, H., Wang, Q., Wang, Y., Zhou, Y., Chen, C., Xiao, M., Slowik, J. G., Brown, S., Cassagnes, L.-E., Daellenbach, K. R., Nussbaumer, T., Geiser, M., Prévôt, A. S. H., El-Haddad, I., Cao, J., Baltensperger, U., and Dommen, J.: Predominance of secondary organic aerosol to particle-bound reactive oxygen species activity in fine ambient aerosol, Atmos. Chem. Phys., 19, 14703–14720, https://doi.org/10.5194/acp-19-14703-2019, 2019.