Skip to main content
NCBI home page
ACS AuthorChoice logoLink to ACS AuthorChoice
. 2021 Feb 17;55(5):2878–2889. doi: 10.1021/acs.est.0c06838

Optical Properties of Secondary Organic Aerosol Produced by Nitrate Radical Oxidation of Biogenic Volatile Organic Compounds

Quanfu He †, Sophie Tomaz ‡, Chunlin Li †, Ming Zhu §,∥, Daphne Meidan †, Matthieu Riva ‡, Alexander Laskin ⊥, Steven S Brown #,▽, Christian George ‡, Xinming Wang §,∥,○, Yinon Rudich †,*
PMCID: PMC8023652  PMID: 33596062

Abstract

graphic file with name es0c06838_0006.jpg

Nighttime oxidation of biogenic volatile organic compounds (BVOCs) by nitrate radicals (NO3·) represents one of the most important interactions between anthropogenic and natural emissions, leading to substantial secondary organic aerosol (SOA) formation. The direct climatic effect of such SOA cannot be quantified because its optical properties and atmospheric fate are poorly understood. In this study, we generated SOA from the NO3· oxidation of a series BVOCs including isoprene, monoterpenes, and sesquiterpenes. The SOA were subjected to comprehensive online and offline chemical composition analysis using high-resolution mass spectrometry and optical properties measurements using a novel broadband (315–650 nm) cavity-enhanced spectrometer, which covers the wavelength range needed to understand the potential contribution of the SOA to direct radiative forcing. The SOA contained a significant fraction of oxygenated organic nitrates (ONs), consisting of monomers and oligomers that are responsible for the detected light absorption in the 315–400 nm range. The SOA created from β-pinene and α-humulene was further photochemically aged in an oxidation flow reactor. The SOA has an atmospheric photochemical bleaching lifetime of >6.2 h, indicating that some of the ONs in the SOA may serve as atmosphere-stable nitrogen oxide sinks or reservoirs and will absorb and scatter incoming solar radiation during the daytime.

1. Introduction

Atmospheric secondary organic aerosols (SOAs) affect radiative forcing by aerosol–radiation interactions and through aerosol–cloud interactions.1,2 Specifically, SOAs contain light-absorbing compounds, also called brown carbon (BrC), and play a significant role in the direct climate forcing on regional and local scales.3,4 Owing to the high emission rates and high reactivities with primary atmospheric oxidants, such as ozone, the hydroxyl radical (OH·), and the nitrate radical (NO3·), vegetation-emitted biogenic volatile organic compounds (BVOCs), such as isoprene (C5H8), monoterpenes (C10H16), and sesquiterpenes (C15H24), are the major contributors to the global SOA burden.5−9

Whereas OH· and ozone (O3) play a key role during daytime atmospheric oxidation, NO3· is a dominant oxidant at night, especially in environments affected by anthropogenic emissions.10 NO3· is formed by the reaction of nitrogen dioxide and O3 and reaches atmospheric concentrations up to hundreds of parts per trillion (ppt).11,12 Field studies have shown that under conditions with moderate to high BVOC levels, NO3· predominantly reacts with BVOCs12 to produce multifunctional compounds such as organic nitrates (ONs).13−16 Because of their semivolatile/low-volatility nature, ONs can partition in the particle phase either by condensing onto pre-existing particles or by forming new SOA particles.13,17,18 Chamber studies have shown that the SOA mass yields from BVOC + NO3· reactions vary between 0.2 and 146% and that the ON molar yields range between 10 and 78%.7 The results from field measurements have also shown that the nocturnal NO3-initiated oxidation of BVOCs contributes a significant fraction to ambient particulate nitrates19−22 and organic aerosols23−26 that influence the air quality, human health, and the climate. Moreover, particle-phase ONs can either release nitrogen oxides (NOx = NO + NO2) back into the atmosphere via further oxidation reactions and photolysis or act as terminal NOx sinks through hydrolysis and particle deposition. Therefore, ONs play essential roles in the atmosphere and biosphere because they affect tropospheric O3 production and the global nitrogen cycle.

Although the oxidation of BVOCs by NO3· represents a critical interaction between anthropogenic and biogenic emissions, the direct radiative effects of the SOA from this process are not well constrained, in part because their optical properties are not yet insufficiently described.27 Whereas most of the existing literature on the optical properties of BVOC-derived SOAs has mainly focused on OH· oxidation or ozonolysis,27−33 studies on the optical properties of the biogenic SOA formed by NO3· oxidation (BSOANO3) are rare. The few studies that examined the BSOANO3 reached partially contradictory conclusions.34−37 For instance, the real part of the refractive index (RI) for the SOA from the NO3· oxidation of β-pinene and limonene was higher than those observed following OH- and ozone-initiated terpene oxidation.35,37 However, the real part of the RI for the SOA from the NO3· oxidation of isoprene seems to be similar to that of OH· and ozone-initiated oxidation.34 Moreover, absorption was not detected for the SOA from the NO3· oxidation of isoprene, β-pinene, and limonene, but significant light absorption at 355 and 405 nm was detected for the SOA formed by NO3·+ α-pinene.36 Washenfelder et al.38 measured aerosol optical properties at a forest site in rural Alabama during the 2013 Southern Oxidant and Aerosol Study (SOAS) campaign. They reported that ∼7% of BrC absorption could be attributed to the less oxidized oxygenated organic aerosol (LO-OOA) that reached a diel maximum at night and was correlated with particle-phase ONs, formed by nighttime reactions between monoterpenes and NO3·.23 These findings suggest that the SOA produced from reactions of NO3· with BVOCs may be a nighttime source of BrC that may affect the direct radiative effect of the SOA through the scattering and absorption of solar radiation. The optical properties of the BSOANO3 and its fate during daytime photooxidation remain unclear.

In this study, the representative BSOANO3 was produced by reactions of the most common BVOCs, such as isoprene, terpenes, and sesquiterpenes, with NO3·. We determined the scattering and absorption optical properties of the BSOANO3 over a very broad wavelength range (315–650 nm) for the first time. These optical properties are needed to understand their potential contributions to direct radiative forcing. We investigated the relationship between the SOA formation mechanism, the SOA’s chemical composition, and the measured optical properties. We show that the absorbing particulate organic nitrates have a lifetime >6 h upon the transition from nighttime to daytime oxidation. This study thus emphasizes the role of this important chemistry in the climate, air quality, and atmospheric nitrogen cycle.

2. Methods

2.1. SOA Generation with NO3· Oxidation

BVOCs (isoprene, monoterpenes (β-pinene and δ3-carene), and sesquiterpenes (α-cedrene, β-caryophyllene, and α-humulene)) were introduced into a glass oxidation flow reactor (OFRNO3, L: 70 cm, ID: 7 cm) from a temperature-controlled glass reservoir. The target mixing ratio of the VOCs was achieved by controlling the flow rate through the glass reservoir and the bath temperature (−50 to +50 °C). The NO3· radical was produced by the thermal decomposition of synthetic N2O5 (Supporting Information (SI), Text S1). The initial mixing ratio of N2O5 was measured by a cavity ring-down system working at 662 nm (Text S2). Pure nitrogen that had been passed through the N2O5 crystal cold trap was mixed with dry synthetic air containing the BVOCs in the OFRNO3 to produce BSOANO3 particles by homogeneous nucleation and condensation following the NO3· oxidation. The produced particles were then subjected to online and offline chemical–physical analysis (Figure S1). The total laminar flow in the reactor was 1.0 L min–1 (Reynolds number ≈ 20) with a corresponding residence time of 162 s. The initial conditions, including the BVOC mixing ratios and N2O5/VOC ratios, are summarized in Table S1.

2.2. Photochemical Aging and Photolysis of the BSOANO3

The BSOANO3 produced in the OFRNO3 from β-pinene and α-humulene was further aged by OH· and photolysis in a potential aerosol mass (PAM) oxidation flow reactor (OFR). Gas-phase species produced in the OFRNO3 were removed by a charcoal denuder before the PAM reactor. OH· was generated by UV photolysis (at 254 nm) of 19.6 ppmv O3 under 37.5% relativ humidity (RH). The total flow rate in the PAM was 3.2 L min–1, with a corresponding residence time of 252 s. The operational details can be found in our previous study.33 OH· exposure (the combination of OH· concentration and residence time) was determined by tracking the decay of SO2 in the PAM reactor. The equivalent OH· aging time was 24 h (assuming a daily average OH· concentration of 1.5 × 106 molecules cm–3). Although the O3 concentration is higher than that of OH·, the much higher reactive uptake coefficient and reactivity of OH· ensure that the OH· plays a major role in the chemical aging process in the PAM reactor. Photolysis experiments were performed in the PAM reactor in the absence of O3 for comparison with the OH· aging experiments. Because the light emission spectrum of the UV lamps inside the PAM reactor is different from the ambient solar spectrum, the photolysis in the PAM reactor is converted to effective photolysis under ambient conditions by considering the actinic flux and the quantum yield of the SOA products. The calculation of the effective photolysis time is briefly described here with more information in the SI (Text S3, Figure S2). The quantum yields for the photolysis reactions of the SOA constitutes are unknown. In the generated SOA, many carbonyl and nitrate groups were detected. Moreover, the extracted absorption spectra (Figure S3) suggest the presence of carbonyl nitrates. (See Section 3.3.) Thus we assume a unified quantum yield of 0.9, as recommended for carbonyl nitrates by previous studies.39,40 The photolysis rate under the experimental conditions is then integrated over the 250–350 nm spectrum by considering the light absorption, quantum yield, and photon flux in the PAM. In addition, solar photolysis rates for the BSOANO3, considering the daily averaged actinic flux under cloudless ground-level conditions (Rehovot, Israel on December 17, 2019, albedo of 0.19), were also estimated. Dividing the photolysis effect (the combined product of the photolysis time and the photolysis rate) in the PAM by the solar photolysis rate yields the effective photolysis time, which was ∼0.8 h.

2.3. Chemical Box Modeling and Photolysis Time Estimation

To track the oxidation process in the OFR, a chemical-box model that includes gas-phase reactions of BVOCs + NO3,41 conversions between NO3· and N2O5, the heterogeneous reactive uptake of NO3· and N2O5,42,43 and wall losses of NO3· and N2O5 was used to investigate the fates of BVOCs, NO3·, and N2O5 in the OFR (Text S4, Tables S2–S4, and Figure S4). Because of the high reaction rates of BVOCs with NO3·, the BVOCs were completely (>99%) consumed in the OFR, except for isoprene (60%), which has a much slower rate constant with NO3 as compared with the other studied BVOCs. The N2O5 loss was dominated by wall loss (34–84%), whereas the thermal dissociation of N2O5 to produce NO3· was also significant (13–64%), as shown in Table S3. For experiments run at a N2O5/VOC ratio of <3, the amount of NO3· or N2O5 taken up by the particles was negligible compared with the consumption of NO3· by VOCs. However, at a high N2O5/VOC ratio (>3), the NO3· and N2O5 uptake by particles became considerable, indicating the importance of the heterogeneous reaction in the reactor. Moreover, the integrated NO3· exposures (NO3 exposure = ∑0t[NO3] dt) throughout the OFR ranged between 5.4 and 64.9 × 1011 molecules cm–3 s, which equals 0.3–3.5 h of ambient exposure by NO3·, assuming a typical concentration of 20 pptv at night.44,45

2.4. Online and Offline Chemical–Physical Characterization of the BSOANO3

The particle size distribution was continuously monitored with a scanning mobility particle sizer (SMPS, TSI) and an aerosol aerodynamic classifier (AAC, Cambustion, U.K.). The ratio of the aerodynamic and mobility size was then used to determine the particle effective density. A high-resolution time-of-flight aerosol mass spectrometer (HR-Tof-AMS, Aerodyne) was employed to measure the nonrefractory components (e.g., organics, nitrate) of the SOA in alternating V and W mode. Elemental ratios (e.g., H/C, O/C, N/C) and the fragment composition were extracted and corrected.46,47 The detected ions in the mass spectra were classified into five categories based on their elemental compositions, namely, hydrocarbon-like (CxHy+), less oxygenated (CxHyO+), more oxygenated (CxHyOz+), nitrogen-containing (CxHyOiNj+) organic components, and nitrogen oxides (NOy+), where x, y, i, and j ≥ 1 and z > 1.

SOA particles were collected on PTFE filters (0.45 μm porosity, 47 mm diameter, Whatman). Filters were stored at −20 °C before analysis. The filters were extracted, and the filtrate was concentrated and analyzed by ultra-high-performance liquid chromatography (UPLC) equipped with a photodiode array (PDA) detector (spectra detection range of 200–800 nm) followed by a Q-Exactive hybrid quadrupole–Orbitrap mass spectrometer (Orbitrap MS) with a standard heated electrospray ionization48 source. The raw data were acquired using Xcalibur (Thermal Scientific) software. The data were then processed with an open-source software toolbox, MZmine 2.39 (http://mzmine.github.io/), to perform peak deconvolution and chromatogram construction. Formula assignments were completed using the following constraints: C ≤ 50, H ≤ 100, N ≤ 4, O ≤ 50, and Na ≤ 1. (The latter is for positive mode only.) Details of the sample preparation, column separation, instrument configurations, and settings of MZmine 2.39 are provided in Text S5.

2.5. Optical Properties Measurement and RI Retrieval

The light extinction by size-selected SOA particles in the solar spectral region (315–650 nm) was measured by a two-channel broadband cavity-enhanced spectrometer (BBCES). The UV channel measures the light extinction between 315 and 350 nm (BBCESUV),49,50 and the visible channel works between 380 and 650 nm (BBCESvis).33 High-reflectivity mirrors (FiveNine Optics, U.S.) were installed in the BBCESvis. The mirror loss measured using N2 and He ranged from 86 to 494 ppm in the wavelength range of 380–650 nm. The low mirror loss ensures high sensitivity and low uncertainty in the aerosol light extinction measurements. The complex refractive index (RI = n + ik) is an intrinsic optical property of a particle. The real (n) and imaginary (k) parts of the complex RI are indicative of scattering and absorption, respectively. The complex RI of the aerosols was retrieved by extinction measurements of several particle sizes (175 to 325 nm with 25 nm steps), assuming sphericity and similar composition for each selected diameter, and by fitting a Mie curve to the measured extinction cross sections at each specific wavelength.28,51−55 In brief, dried particles from the OFR were sampled after a VOC denuder. Particles were size-selected with an AAC, thus yielding a monodispersed particle size distribution. The monodispersed particles were directed into a photoacoustic (404 nm)–cavity ring-down spectrometer (404 nm)–broadband cavity-enhanced spectrometer (PAS-CRDS-BBCES) system and counted by a condensation particle counter (CPC, model 3752, TSI). The retrieval algorithm was limited to searching for n ≥ 1 and k ≥ 0.

3. Results and Discussion

3.1. Bulk Characterization of the BSOANO3 Using HR-Tof-AMS

The oxidation reactions of isoprene and terpenes with NO3· occur almost exclusively by the addition of the NO3· to the C=C double bond to form the most substituted nitrooxyalkyl radical.56,57 This nitrooxyalkyl radical reacts with O2 to create β-nitrooxyperoxy radical (RO2·) that further reacts with NO3·, hydroperoxyl radical (HO2·), and another RO2· to produce hydroxyl nitrate, carbonyl nitrate, and nitrooxyperoxide.41 Large RO2· species can undergo autoxidation to produce highly oxidized molecules58−61 or produce dimers through bimolecular reactions with another RO2·.62,63 The HR-Tof-AMS data of the SOA generated in this study show a high intensity (4.1–24.7%) at m/z 43 (C2H3O+, characteristic fragment of carbonyl compounds) and contain a considerable fraction (1.8–3.9%) of nitrogen-containing fragments (CxHyOiN+) (Figure 1 and Table S1), indicating that the production of carbonyls and ONs is favored during the NO3· oxidation of BVOCs, which is consistent with the known oxidation mechanism.41 Weak mass peaks at m/z 44 (CO2+) from carboxyl/acyl peroxide groups64 were detected (0.6–4.0%, Figure 1 and Table S1). These mass spectra of the SOA from the NO3· oxidation of BVOCs consist of a prominent CxHy+ ion signal (an indication of the hydrocarbon-like organic aerosol (HOA)) and CxHyO+ ion signals (a sign of carbonyl compounds), whereas the signature of higher-generation oxidation products (indicated by CxHyOz+ ions) is observed at trace levels. These features are common in the ambient semivolatile oxygenated organic aerosols (SV-OOAs) or LO-OOAs.23,64−67

Figure 1.

Figure 1

Open in a new tab

Chemical composition of the BSOANO3 measured by HR-Tof-AMS. The pie charts show the bulk chemical information, including organic-related fragments (grouped as CxHy+, CxHyO+, CxHyOz+, CxHyOiNj+, and NOy+, where x, y, z, and j ≥ 1, i ≥ 0). Large portions of hydrocarbon-like (indicated by CxHy+), less oxygenated fragments (indicated by CxHyO+), and nitrogen-containing fractions (indicated by CxHyOiNj+ and NOy+) are observed. The boxed legend is for the mass spectra, whereas the bold legend belongs to the pie chart. Ions of CxHyN, CxHyON, and CxHyOzN in the mass spectra are categorized to CxHyOiNj+ in the pie chart.

Nitrogen-containing ions (CxHyOiNj+, NO+, and NO2+) comprise ∼17% (11–25%) of the combined organic and nitrate signals and are detected mainly as NO+ and NO2+ ions (7–23%) with a small amount of CxHyOiNj+ ions (2–4%) for all of the generated BSOANO3. In this study, the reactions were performed under dry conditions (RH < 5%), and no ammonium was detected in the SOA; therefore, nitrogen-containing fragments are predominantly from ONs. The characteristic fragment intensity ratio of NO+/NO2+ has been frequently used as an indicator of particulate organic nitrate, as this ratio is much higher for organic nitrates (usually assumed to be 10) than the ratio measured for inorganic nitrates, as determined by measuring it for NH4NO3.19,68−70 The NO+/NO2+ ratios in the mass spectra of the SOA ranged from 4.0 to 9.6 in this study, comparable to those observed for the SOA from the NO3· oxidation of isoprene, β-pinene, δ3-carene, and limonene.15,70−74 These ratios are higher than those of inorganic nitrates (2.2 for NH4NO3), further supporting the formation of ON products. The N/C ratio of the SOA formed from the β-pinene + NO3 reaction averaged 0.077, which is in good agreement with the reported values of 0.070 to 0.076 in previous studies.15,74,75

3.2. Complex Refractive Index of the Generated BSOANO3

Only a few previous studies have investigated the RI of the SOA produced from NO3· oxidation.35−37Figure 2 shows the RI of the BSOANO3 across most of the solar wavelength range (315–650 nm). A comparison of our results and the literature data is shown in Figure S5. To the best of our knowledge, this is the first set of wavelength-resolved RI results for the BSOANO3 over such a wide wavelength range based on online measurements. The real part of the RI (n) of the BSOANO3 in this study varied between 1.43 and 1.55. The real RI for the generated SOA exhibits a slight spectral dependence with n values that decrease with increasing wavelength. This weak wavelength dependence is similar to that observed for the SOA from the OH· oxidation of β-pinene33 and the ozonolysis of monoterpenes.31 Moreover, the results from the BBCES are consistent with those from an independent CRD measurement. The value of n at 404 nm for the SOA of isoprene + NO3 (1.472 ± 0.007) from our study is similar to those (1.455–0.023+0.023 to 1.468–0.027) measured for the SOA from isoprene + O3 + NOx in the presence/absence of sulfur dioxides.34 However, the values of n at 532 nm for the SOA from β-pinene + NO3 (1.486 ± 0.001) and δ3-carene + NO3 (1.493 ± 0.001) are much lower than that (1.578) of limonene + NO3,35 indicating that the real RI of the BSOANO3 highly depends on the VOC precursor. Varma et al.37 studied the NO3-initiated oxidation of β-pinene under dry conditions using the BBCES at the SAPHIR atmospheric simulation chamber. They determined an n value of 1.61 ± 0.03 between 655 and 687 nm, assuming no absorption. In our study, the wavelength range was limited to 650.7 nm. The n value for the BSOANO3 from β-pinene at this wavelength is 1.474 (±0.001), which is substantially lower than those from the SAPHIR experiments. The SAPHIR experiments were conducted at much lower VOC levels (<18 ppbv) and for a longer period (∼1 h) compared with this study (>40 ppbv, 162 s). These differences in the experimental conditions may lead to a differences in the SOA formation that will further affect the real RI.

Figure 2.

Figure 2

Open in a new tab

Wavelength-dependent optical properties of the BSOANO3. The real part (a) and imaginary part (b) decrease with increasing wavelength. The k is observed only at the deep UV wavelength range. (c) Single scattering albedo (SSA) values were calculated for 200 nm spherical particles. Data for β-pinene, β-caryophyllene, and the α-humulene-derived SOA are taken from experiments with a N2O5/VOC ratio of 1.2, 10.7, and 8.8, respectively. The results of isoprene, δ3-carene, and α-cedrene are obtained under a N2O5/VOC ratio of 1.3, 1.9, and 5.8, respectively.

Previous studies determined a near-zero imaginary part of the RI (imaginary RI, k) of the SOA produced by the photooxidation/ozonolysis/OH oxidation of BVOCs under NOx-free conditions for the atmospherically relevant wavelength region (λ > 300 nm), especially in the visible range.3,27,32,33,51 In this study, we determined the optical properties of the BSOANO3 in the short UV wavelength range (315–350 nm) using our unique UV channel (BBCESUV). Most of the generated SOA absorbs slightly in the deep UVA wavelength range, and k decreases with increasing wavelength (Figure 2 and Table S5), which is the typical behavior of BrC. The k values obtained from all of the oxidation experiments are 0.003 to 0.046 at 316 nm and 0.001 to 0.039 at 330 nm. Above 390 nm, very weak light absorption was detected, in line with previous findings for the BSOANO3.34,35,37 The retrieved k in the UV range is similar to that observed for the SOA produced by the photooxidation of aromatic compounds (e.g., toluene and m-xylene) and higher than that of the SOA generated by the ozonolysis of α/β-pinene.31,76 The k of the BSOANO3 obtained in this study is much lower than that for the ammonia-aged biogenic SOA51 and biomass burning aerosols (Figure S5).38,77−80 Recently, the optical properties of the SOA from the NO3· oxidation of unsaturated heterocyclic VOCs were studied.81 The values of k for pyrrole and the thiophene-derived SOA range between 0.002 and 0.017 at 375 nm. These values are higher than those measured for the BSOANO3 in this study. Previous studies for isoprene + NO3 have reported an k value of 0.0001 at 375 nm when sulfur dioxide is added during the oxidation process.34 In this study, the k value of the SOA from isoprene + NO3 is 0.005 (±0.006) at 349.4 nm, and it is essentially zero in the longer wavelength range (380–650 nm). The imaginary RI of the BSOANO3 from α-humulene is the largest among all of the studied systems. As discussed in Sections 3.3–3.5, the absorption is controlled by the ONs in the SOA, and ONs that have a carbonyl-adjacent nitrate group exhibit stronger absorption compared with other types of ONs. The high N2O5/VOC ratio in the α-humulene + NO3· experiment (8.8) favors the formation of ONs. Moreover, α-humulene has three substituted C=C bonds (two, one, one, one, and two for isoprene, β-pinene, δ3-carene, α-cedrene, β-caryophyllene, respectively) that can form stable (and do not favor cyclize reactions) ONs with a carbonyl adjacent to the nitrate group. This results in a stronger absorption in the BSOANO3 from α-humulene as compared with the other types of BSOANO3.

The single scattering albedo (SSA) (SSA = scattering/extinction) is frequently used in climate models. The SSA data for the BSOANO3 in this study were calculated for 200 nm particles based on the Mie theory using the retrieved refractive index. The SSA is 1 for all BSOANO3 above 425 nm. In the UV ranges, the SSA increases from 0.80 to 1 with increasing wavelength. These values are higher than those obtained for the SOA produced from aromatics32,76,82 and the aerosol derived from biomass burning.80,83 Overall, the BSOANO3 is not a significant BrC contributor. However, it does absorb substantially between 280 and 300 nm, meaning it is photochemically active in the UVA range, which likely induces condensed-phase photochemistry.

3.3. Linking Light Absorption with Chromophores

The nighttime reactions of BVOCs with NO3· lead to the formation of secondary BrC, which absorbs at short wavelengths. Therefore, it is essential to identify the compounds that are responsible for the observed absorption. Figure 3 shows the UV–vis chromatograms at 290 nm (blank corrected) as detected by the ultraperformance liquid chromatography–photodiode array (UPLC-PDA) performed in parallel with heated electrospray ionization/high-resolution mass spectrometry (HESI/HRMS). We present absorption at 290 nm to provide a better signal-to-noise ratio. Significant absorption was observed at a retention time (RT) of 9.0 min in the BSOANO3 from β-pinene. High abundances of monomers and dimers with formulas of C10H13–17O5,6 and C19,20H28,31N1,2O10–12 were found in the HESI/HRMS chromatograms. The UV–vis absorption peak at ∼290 nm, which is the absorption feature of carbonyls or ONs,84,85 is coincident with the result from HR-Tof-AMS in that large amounts of carbonyls or ONs were produced in the BSOANO3. We extracted the wavelength-dependent absorption spectra for the chromatograms shown in Figure 3 and compared them to those of typical nitrate-containing organics and carbonyls (Figure S3). The spectra obtained from the BSOANO3 showed an absorption maximum at ∼290 nm within the wavelength range of 240–340 nm, which is similar to that of carbonyls and organic nitrates. This further supports the formula’s assignment from the mass spectrometer and illustrates that carbonyl ONs are responsible for light absorption, although it is not possible to differentiate the contribution of each compound due to their overlapping elution times in the UPLC. In the other types of BSOANO3 studied, the light absorption was attributed to the most abundant ON dimers and oligomers. Interestingly, two C15H25NO6 isomers in the BSOANO3 from α-humulene are potential light -absorbers, whereas only one of the four isomers of C15H24N2O9, the dominant species in the mass spectra, showed detectable light absorption (Figure S6). This indicates that different isomers can have quite different lifetimes regarding atmospheric photolysis. Only a few light-absorbing species with weak absorption were identified in the BSOANO3 from β-caryophyllene (Figure 3e), consistent with the result from the online BBCES measurements.

Figure 3.

Figure 3

Open in a new tab

Possible formulas of absorbing compounds detected in the BSOANO3 by HPLC-PDA-HESI/HRMS. ONs are responsible for the absorption peaks observed by the PDA. Data for the β-pinene-, β-caryophyllene-, and α-humulene-derived SOAs are taken from experiments with a N2O5/VOC ratio of 1.2, 10.7, and 8.8, respectively.

3.4. Influence of the N2O5/VOC Ratio on the Chemical Composition and RI

Faxon et al.14 measured the chemical composition of the SOA from the NO3· oxidation of limonene using a high-resolution time-of-flight chemical ionization mass spectrometer combined with a filter inlet for gases and aerosols to measure. They found that the chemical composition of the SOA (e.g., thermally unstable dimers) changed dramatically with the initial N2O5/limonene ratio. In this study, we produced the SOA from β-pinene, β-caryophyllene, and α-humulene at different N2O5/VOC ratios (Table S1). Under higher initial N2O5/VOC ratios, more NO3· was involved in the reaction with BVOCs and intermediates or taken up by particles to react with organic species (Table S4). Thus the SOA contains more nitrate groups, as was observed by HR-Tof-AMS (Figure 4a). This was also confirmed by the AMS fragment analysis, where the contribution of NOy+, which originated from ONs in the SOA, increased with the initial N2O5/VOC (Figure S7). The studied terpenes have C=C double bonds with more than one ring. Thus the first-generation oxidation products from NO3·-initiated oxidation may still contain a C=C double bond that can further react with NO3· to generate products with multiple nitrate groups. The RI of the SOA also changed under different initial N2O5/VOC ratios, with a higher real part and imaginary part of the RI under higher N2O5/VOC ratios (Figure S8).

Figure 4.

Figure 4

Open in a new tab

Influence of the initial N2O5/VOC ratio on the chemical–physical properties of the BSOANO3 from β-pinene (○), β-caryophyllene (△), and α-humulene (□). The symbol’s color indicates the initial N2O5/VOC ratio, and the symbol’s size in panel a represents the effective particle density. With the increasing initial N2O5/VOC ratio, the nitrate fraction (fNO3) and the particle’s effective density (a), the elemental ratios (b), the real refractive index at 404 nm (c), and the imaginary refractive index at 316 and 330 nm (d) increased.

Both the H/C and O/C ratios, the particle effective density, and the nitrate fraction (fNO3) in the SOA observed by HR-Tof-AMS increased with increasing N2O5/VOC ratios, as shown in Figure 4b–d, confirming the functionalization (e.g., −OH or −OOH addition to the C=C bonds) during the oxidation by NO3·. The Lorentz–Lorenz relationship (Inline graphic) correlates the real RI (n) to the mean polarizability (α), the particle effective density (ρ), and the average molecular weight (MW) of the SOA. The mean polarizability can be estimated by the additive group contribution method.86,87 The enhanced functionalization under higher N2O5/VOC ratios significantly increases the H/C and O/C ratios and the nitrate fraction and therefore increases the mean polarizability of the SOA, in combination with the increased effective density, causing an increase in the real RI of the BSOANO3 under higher N2O5/VOC ratios. HPLC-PDA-HESI/HRMS results have revealed that ONs are responsible for the observed light absorption. Under higher initial N2O5/BVOC ratio conditions, the fNO3 of the produced SOA is higher, indicating more abundant ONs in the SOA. As a result, a larger imaginary RI is expected. In urban conditions, the NO3· production rate is enhanced, whereas BVOC emissions can be relatively lower. Thus the produced BSOA may show more light-absorbing ability over and downwind of cities.88

3.5. Optical Properties Evolution upon Photochemical Aging

Chemical characterization shows that ONs comprise a significant fraction of the light-absorbing BSOANO3. Therefore, it is important to understand how the optical properties change during daytime OH-dominated oxidation. To address this important question, we exposed the monoterpene (β-pinene) and sesquiterpene (α-humulene) BSOANO3 to an equivalent of 1 day of aging by OH· in a PAM OFR. As shown in Table S6, a slight decrease in the fNO3 was observed (0.201 to 0.196 and 0.206 to 0.192 for β-pinene and α-humulene, respectively), indicating that the particulate ONs are resistant to OH· aging, which is consistent with previous findings for the BSOANO3 from β-pinene.15 For the BSOANO3 from β-pinene, whereas the O/C ratio of the OH·-aged SOA increased slightly, the H/C ratio decreased, indicating the H-abstraction reaction during OH· aging. Upon OH· aging of the BSOANO3 from α-humulene, a slight increase in the H/C (∼0.005) and O/C ratios (by 0.022) was observed, indicating functionalization (OH· addition), possibly due to the remaining unsaturated C=C bonds in the SOA, which favors the addition of functional groups.

In Figure 5, we show the RI evolution from photochemical aging. The real part at 315.3, 330.3, 349.3, 404.4, and 599.8 nm and the imaginary part at 315.3, 330.3, and 349.3 nm are highlighted. For the BSOANO3 from β-pinene, the real RI decreased slightly when the SOA was processed with photolysis and photochemical aging, whereas no significant change in the imaginary RI was observed. For the BSOANO3 from α-humulene, the real RI of the SOA increased during OH· aging, and it is resilient to photolysis. The imaginary RI decreased during both the photolysis and the OH· aging process. Therefore, the SSA for 200 nm particles increased. For the BSOANO3 from β-pinene, the real RI decreased slightly, possibly due to the loss of ON moieties that efficiently scatter light. The absorption of the SOA is linked to specific ONs (e.g., C 10H13–17NO5,6 and C19,20H28,31N1,2O10–12), as shown in Figure 3. Because of the deactivation of the C–H bonds by adjacent functional groups, these highly functionalized ONs have fewer H–C bonds available for H abstraction by OH· oxidation, making them more resistant than less functionalized compounds. Thus the imaginary RI does not significantly change during the OH· aging experiments. Moreover, the interaction between the carbonyl and the nitrate functional groups will induce strong light absorption. A previous study by Draper et al. has found that ONs with a carbonyl adjacent to the nitrate group can be produced through left scission reactions of nitroxyalkoxyl radicals that are produced by the NO3· radical oxidation of unsaturated VOCs.13 The β-pinene molecule has only one substituted C=C double bond to form products with a carbonyl adjacent to the nitrate group. Moreover, these products rapidly cyclize and further react in particles to form acetal heterodimers and heterotrimers, leading to a loss of the carboxyl adjacent to the nitrate groups (Figure S9).57 Thus no significant strong absorbing species will be produced in the BSOANO3 from β-pinene. Moreover, in the ON produced from the NO3· oxidation of β-pinene, the carbonyl group is further away from the nitrate functional group, or there is a hydroxyl functional group adjacent the nitrate functional group.57,74 The lack of interaction between carbonyl and nitrate functional groups seems to induce negligible light absorption. This weak light-absorbing ability of the BSOANO3 also suggests that its photolysis will be insignificant, which is in line with the previous finding that the ON fraction of the BSOANO3 from β-pinene was resistant to photochemical aging.15 As a result of the significant decrease in the real part and the small change in the imaginary part upon OH· aging, the SSA decreased in the UVA range, indicating that the aged SOA can have a relatively stronger warming effect. The α-humulene molecule has three substituted C=C double bonds that form products with a carbonyl adjacent to the nitrate group. The carbonyls adjacent to the nitrate groups are further away from the hydroxyl group, which does not favor the cyclize process, stabilizing in the particle phase. The coupling of these two functional groups in the BSOANO3 from α-humulene can enhance the light absorption, as confirmed by the relatively high imaginary RI, resulting in the higher photolysis efficiency of ONs. The photolysis proceeds by releasing NO2 and forming compounds with fewer or even no nitrate groups. Photolysis at UVA will also decompose carbonyls, which would have an additional photobleaching effect. Thus upon photolysis, both the real part and the imaginary part of the RI decreased, resulting in an overall increase in the SSA. On the basis of the change in absorption, we calculated the photolysis lifetime of absorbing ON in the BSOANO3 to be 6.2 h (Text S3), assuming no phase separation, which may affect the aging. Assuming no synergetic effect between photolysis and OH· aging and excluding the photolysis-induced decrease in absorption, the OH· aging also bleached the particles with a lifetime of 38.8 days. For the α-humulene-derived BSOANO3, bleaching by photochemical aging (including OH· aging and photolysis) is governed by photolysis, and the lifetime is ∼6 h. These results from the β-pinene and α-humulene aging experiments indicate that the effect of photochemical aging on the optical properties (refractive index and SSA) of the BSOANO3 largely depends on the specific chemical nature of the ONs and their precursors, leading to a more complicated picture than just “bleaching” or “browning”.

Figure 5.

Figure 5

Open in a new tab

Modification of the RI and single scattering albedo (SSA) of the BSOANO3 by OH· aging and photolysis. (A,B) Evolution of the broadband RIs of the BSOA from the NO3· oxidation of β-pinene and α-humulene after 24 h of equivalent ambient OH· exposure time or 1.7 × 1014 photons cm–2 photolysis at 254 nm. (C) SSA transformations for 200 nm SOA particles at UV wavelengths (315–349 nm). Changes in the RI and SSA at 315.3 (purple), 330.3 (light blue), 349.3 (blue), 404.4 (cyan), and 599.8 (red) are displayed as lines.

4. Atmospheric Implications

The study provides the chemical composition and optical properties of the SOA produced during the NO3· oxidation of terpenoids. The BBCES-CRD measurements show that the nighttime reactions studied here form BrC, which weakly absorbs light in the UVA range. According to the framework recently introduced by Saleh et al.,89 the produced BSOANO3 falls into the category of very weakly absorptive BrC. The UPLC-PDA-HRMS analysis confirmed that ONs are responsible for light absorption. In urban and suburban areas that are affected by anthropogenic pollution and high BVOC emissions, the high NOx and O3 promote NO3· production. This could also result in a high NO3·/VOC ratio, which favors BrC that contains a high fraction of ONs. Although the light absorption of the BSOANO3 is weak, the SOA formation from the nighttime NO3· oxidation of BVOCs is efficient, especially in regions where massive anthropogenic emissions mix with BVOCs. Therefore, the BSOANO3 can have a measurable impact on the aerosol UVA absorption, which could further affect the climate and air quality on a regional scale.

The BSOANO3 from α-humulene has an equivalent photolysis lifetime longer than 6.2 h (Text S3). Because of their weak light-absorbing properties, the photolysis of the ONs in the β-pinene BSOANO3 is negligible (Figure 5). Previous studies have tested the bulk hydrolysis properties of the BSOANO3 from α- and β-pinene.16,74 The hydrolysis lifetime varies between 0.02 and 8.8 h, depending on the precursor VOCs, oxidant type, aerosol acidity, relative humidity, and more. Although the lifetime is short, the ON from NO3· oxidation has a low hygroscopicity, and only a small fraction (≤17%) can undergo hydrolysis.16 Taking all of these factors into consideration, we suggest that the BSOANO3 generated from β-pinene and α-humulene at night would survive into the morning hours or longer and would scatter and absorb the incoming solar radiation and sequester NOx. These results indicate that ONs produced from the NO3· oxidation of β-pinene and α-humulene may serve as NOx reservoirs or permanent NOx sinks in the atmosphere, which is consistent with previous findings.15 We note that previous studies by Nah et al. have found that the particle-phase ONs in the BSOANO3 from α-pinene evaporate during photochemical aging.15 The significant photolysis of the α-pinene BSOANO3 could dramatically change its optical properties, as it behaves differently compared with the BSOANO3 from α-humulene and β-pinene. These results indicate that ONs in the BSOANO3 produced from terpenes can serve as either temporary or permanent NOx sinks depending on the precursor. This finding has significant implications for NOx and O3 budgets in areas with high emissions of monoterpenes and sesquiterpenes, such as the Southeastern United States, Northern Europe, and Southeast Asia. We suggest incorporating these processes into the current modeling strategies to improve NOx and O3 simulations.

This study focused on the ON production by the NO3· oxidation of BVOCs, the optical properties of the resulting BSOA, and the evolution of their chemical and physical properties during the transition from night to day. The link between the BSOANO3 formation mechanism, its chemical and physical properties, and the dynamic evolution was illustrated for both laboratory simulations and ambient aerosols. Photolysis and OH· aging were studied here under low relative humidity (37.5%) conditions, and the possible role of the hydrolysis of the ONs was not investigated. It is also noted that isomers with the same formula have different light-absorbing properties and lifetimes. Therefore, isomer-specific studies may be helpful for understanding the bulk chemical and physical properties (e.g., hydrolysis and oxidation) of ONs and the SOA. Obviously, RO2· chemistry plays a role in determining the changes to the chemical and optical properties of the SOA. In this study, we focused on one set of (extreme) conditions. More detailed studies and additional modeling efforts will be conducted to understand how different RO2· regimes affect these changes and how these translate to different atmospheric chemical regimes.

Acknowledgments

This research was partially supported by the Israel Science Foundation (ISF) (no. 3205/19), the National Natural Science Foundation of China (NSFC) (grant no. 41961144029/41530641), the US-Israel Binational Science Foundation (BSF grant no. 2016093), the Israel Ministry of Science (Maimonides program grant no. 3-14010), and the University of Lyon through the Breakthrough project WANTED. Q.H. is supported by the Koshland Foundation and the Center for Planetary Sciences, Weizmann Institute of Science.

Supporting Information Available

The Supporting Information is available free of charge at https://pubs.acs.org/doi/10.1021/acs.est.0c06838.

  • Additional description of methods; additional tables showing details of the SOA generation, chemical and optical results of the BSOANO3, and the model simulation results in the OFR; additional figures showing the experimental setup, absorption spectra of ONs and carbonyls from the literature and those of compounds of interest in the BSOANO3, RI results for the BSOANO3 and from the literature, and the influence of the N2O5/VOC ratio on the chemical composition and RI (PDF)

The authors declare no competing financial interest.

Supplementary Material

es0c06838_si_001.pdf (2.5MB, pdf)

References

  1. Boucher O., Randall D.; Artaxo P.; Bretherton C.; Feingold G.; Forster P.; Kerminen V.-M.; Kondo Y.; Liao H.; Lohmann U.; Rasch P.; Satheesh S. K.; Sherwood S.; Stevens B.; Zhang X. Y.. Clouds and Aerosols. In Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change; Cambridge University Press: New York, 2013.
  2. Seinfeld J. H.; Bretherton C.; Carslaw K. S.; Coe H.; DeMott P. J.; Dunlea E. J.; Feingold G.; Ghan S.; Guenther A. B.; Kahn R.; Kraucunas I.; Kreidenweis S. M.; Molina M. J.; Nenes A.; Penner J. E.; Prather K. A.; Ramanathan V.; Ramaswamy V.; Rasch P. J.; Ravishankara A. R.; Rosenfeld D.; Stephens G.; Wood R. Improving our fundamental understanding of the role of aerosol–cloud interactions in the climate system. Proc. Natl. Acad. Sci. U. S. A. 2016, 113 (21), 5781–5790. 10.1073/pnas.1514043113. [DOI] [PMC free article] [PubMed] [Google Scholar]
  3. Laskin A.; Laskin J.; Nizkorodov S. A. Chemistry of Atmospheric Brown Carbon. Chem. Rev. 2015, 115 (10), 4335–4382. 10.1021/cr5006167. [DOI] [PubMed] [Google Scholar]
  4. Feng Y.; Ramanathan V.; Kotamarthi V. R. Brown carbon: a significant atmospheric absorber of solar radiation? Atmos. Atmos. Chem. Phys. 2013, 13 (17), 8607–8621. 10.5194/acp-13-8607-2013. [DOI] [Google Scholar]
  5. 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 T. F.; Monod A.; Prevot A. S. H.; Seinfeld J. H.; Surratt J. D.; Szmigielski R.; Wildt J. The formation, properties and impact of secondary organic aerosol: current and emerging issues. Atmos. Chem. Phys. 2009, 9 (14), 5155–5236. 10.5194/acp-9-5155-2009. [DOI] [Google Scholar]
  6. Kanakidou M.; Seinfeld J. H.; Pandis S. N.; Barnes I.; Dentener F. J.; Facchini M. C.; Van Dingenen R.; Ervens B.; Nenes A.; Nielsen C. J.; Swietlicki E.; Putaud J. P.; Balkanski Y.; Fuzzi S.; Horth J.; Moortgat G. K.; Winterhalter R.; Myhre C. E. L.; Tsigaridis K.; Vignati E.; Stephanou E. G.; Wilson J. Organic aerosol and global climate modelling: a review. Atmos. Chem. Phys. 2005, 5, 1053–1123. 10.5194/acp-5-1053-2005. [DOI] [Google Scholar]
  7. Ng N. L.; Brown S. S.; Archibald A. T.; Atlas E.; Cohen R. C.; Crowley J. N.; Day D. A.; Donahue N. M.; Fry J. L.; Fuchs H.; Griffin R. J.; Guzman M. I.; Herrmann H.; Hodzic A.; Iinuma Y.; Jimenez J. L.; Kiendler-Scharr A.; Lee B. H.; Luecken D. J.; Mao J. Q.; McLaren R.; Mutzel A.; Osthoff H. D.; Ouyang B.; Picquet-Varrault B.; Platt U.; Pye H. O. T.; Rudich Y.; Schwantes R. H.; Shiraiwa M.; Stutz J.; Thornton J. A.; Tilgner A.; Williams B. J.; Zaveri R. A. Nitrate radicals and biogenic volatile organic compounds: oxidation, mechanisms, and organic aerosol. Atmos. Chem. Phys. 2017, 17 (3), 2103–2162. 10.5194/acp-17-2103-2017. [DOI] [PMC free article] [PubMed] [Google Scholar]
  8. Heald C. L.; Jacob D. J.; Park R. J.; Russell L. M.; Huebert B. J.; Seinfeld J. H.; Liao H.; Weber R. J. A large organic aerosol source in the free troposphere missing from current models. Geophys. Res. Lett. 2005, 32 (18), L18809. 10.1029/2005GL023831. [DOI] [Google Scholar]
  9. Goldstein A. H.; Galbally I. E. Known and unexplored organic constituents in the earth’s atmosphere. Environ. Sci. Technol. 2007, 41 (5), 1514–1521. 10.1021/es072476p. [DOI] [PubMed] [Google Scholar]
  10. Edwards P. M.; Aikin K. C.; Dube W. P.; Fry J. L.; Gilman J. B.; de Gouw J. A.; Graus M. G.; Hanisco T. F.; Holloway J.; Hübler G.; Kaiser J.; Keutsch F. N.; Lerner B. M.; Neuman J. A.; Parrish D. D.; Peischl J.; Pollack I. B.; Ravishankara A. R.; Roberts J. M.; Ryerson T. B.; Trainer M.; Veres P. R.; Wolfe G. M.; Warneke C.; Brown S. S. Transition from high- to low-NOx control of night-time oxidation in the southeastern US. Nat. Geosci. 2017, 10 (7), 490–495. 10.1038/ngeo2976. [DOI] [Google Scholar]
  11. Brown S. S.; Dubé W. P.; Peischl J.; Ryerson T. B.; Atlas E.; Warneke C.; de Gouw J. A.; te Lintel Hekkert S.; Brock C. A.; Flocke F.; Trainer M.; Parrish D. D.; Feshenfeld F. C.; Ravishankara A. R. Budgets for nocturnal VOC oxidation by nitrate radicals aloft during the 2006 Texas Air Quality Study. J. Geophys. Res. Atmos. 2011, 116 (D24), D24305. 10.1029/2011JD016544. [DOI] [Google Scholar]
  12. Brown S. S.; Stutz J. Nighttime radical observations and chemistry. Chem. Soc. Rev. 2012, 41 (19), 6405–6447. 10.1039/c2cs35181a. [DOI] [PubMed] [Google Scholar]
  13. Draper D. C.; Myllys N.; Hyttinen N.; Møller K. H.; Kjaergaard H. G.; Fry J. L.; Smith J. N.; Kurtén T. Formation of Highly Oxidized Molecules from NO3 Radical Initiated Oxidation of Δ-3-Carene: A Mechanistic Study. ACS Earth and Space Chem. 2019, 3 (8), 1460–1470. 10.1021/acsearthspacechem.9b00143. [DOI] [Google Scholar]
  14. Faxon C.; Hammes J.; Le Breton M.; Pathak R. K.; Hallquist M. Characterization of organic nitrate constituents of secondary organic aerosol (SOA) from nitrate-radical-initiated oxidation of limonene using high-resolution chemical ionization mass spectrometry. Atmos. Chem. Phys. 2018, 18 (8), 5467–5481. 10.5194/acp-18-5467-2018. [DOI] [Google Scholar]
  15. Nah T.; Sanchez J.; Boyd C. M.; Ng N. L. Photochemical Aging of α-pinene and β-pinene Secondary Organic Aerosol formed from Nitrate Radical Oxidation. Environ. Sci. Technol. 2016, 50 (1), 222–231. 10.1021/acs.est.5b04594. [DOI] [PubMed] [Google Scholar]
  16. Takeuchi M.; Ng N. L. Chemical composition and hydrolysis of organic nitrate aerosol formed from hydroxyl and nitrate radical oxidation of α-pinene and β-pinene. Atmos. Chem. Phys. 2019, 19 (19), 12749–12766. 10.5194/acp-19-12749-2019. [DOI] [Google Scholar]
  17. Lee S.-H.; Young L.-H.; Benson D. R.; Suni T.; Kulmala M.; Junninen H.; Campos T. L.; Rogers D. C.; Jensen J. Observations of nighttime new particle formation in the troposphere. J. Geophys. Res. 2008, 113 (D10), D10210. 10.1029/2007JD009351. [DOI] [Google Scholar]
  18. Berkemeier T.; Ammann M.; Mentel T. F.; Pöschl U.; Shiraiwa M. Organic Nitrate Contribution to New Particle Formation and Growth in Secondary Organic Aerosols from α-Pinene Ozonolysis. Environ. Sci. Technol. 2016, 50 (12), 6334–6342. 10.1021/acs.est.6b00961. [DOI] [PubMed] [Google Scholar]
  19. Kiendler-Scharr A.; Mensah A. A.; Friese E.; Topping D.; Nemitz E.; Prevot A. S. H.; Äijälä M.; Allan J.; Canonaco F.; Canagaratna M.; Carbone S.; Crippa M.; Dall Osto M.; Day D. A.; De Carlo P.; Di Marco C. F.; Elbern H.; Eriksson A.; Freney E.; Hao L.; Herrmann H.; Hildebrandt L.; Hillamo R.; Jimenez J. L.; Laaksonen A.; McFiggans G.; Mohr C.; O’Dowd C.; Otjes R.; Ovadnevaite J.; Pandis S. N.; Poulain L.; Schlag P.; Sellegri K.; Swietlicki E.; Tiitta P.; Vermeulen A.; Wahner A.; Worsnop D.; Wu H.-C. Ubiquity of organic nitrates from nighttime chemistry in the European submicron aerosol. Geophys. Res. Lett. 2016, 43 (14), 7735–7744. 10.1002/2016GL069239. [DOI] [Google Scholar]
  20. Lee B. H.; Mohr C.; Lopez-Hilfiker F. D.; Lutz A.; Hallquist M.; Lee L.; Romer P.; Cohen R. C.; Iyer S.; Kurtén T.; Hu W.; Day D. A.; Campuzano-Jost P.; Jimenez J. L.; Xu L.; Ng N. L.; Guo H.; Weber R. J.; Wild R. J.; Brown S. S.; Koss A.; de Gouw J.; Olson K.; Goldstein A. H.; Seco R.; Kim S.; McAvey K.; Shepson P. B.; Starn T.; Baumann K.; Edgerton E. S.; Liu J.; Shilling J. E.; Miller D. O.; Brune W.; Schobesberger S.; D’Ambro E. L.; Thornton J. A. Highly functionalized organic nitrates in the southeast United States: Contribution to secondary organic aerosol and reactive nitrogen budgets. Proc. Natl. Acad. Sci. U. S. A. 2016, 113 (6), 1516–1521. 10.1073/pnas.1508108113. [DOI] [PMC free article] [PubMed] [Google Scholar]
  21. Huang W.; Saathoff H.; Shen X.; Ramisetty R.; Leisner T.; Mohr C. Chemical Characterization of Highly Functionalized Organonitrates Contributing to Night-Time Organic Aerosol Mass Loadings and Particle Growth. Environ. Sci. Technol. 2019, 53 (3), 1165–1174. 10.1021/acs.est.8b05826. [DOI] [PubMed] [Google Scholar]
  22. Ayres B. R.; Allen H. M.; Draper D. C.; Brown S. S.; Wild R. J.; Jimenez J. L.; Day D. A.; Campuzano-Jost P.; Hu W.; de Gouw J.; Koss A.; Cohen R. C.; Duffey K. C.; Romer P.; Baumann K.; Edgerton E.; Takahama S.; Thornton J. A.; Lee B. H.; Lopez-Hilfiker F. D.; Mohr C.; Wennberg P. O.; Nguyen T. B.; Teng A.; Goldstein A. H.; Olson K.; Fry J. L. Organic nitrate aerosol formation via NO3 + biogenic volatile organic compounds in the southeastern United States. Atmos. Chem. Phys. 2015, 15 (23), 13377–13392. 10.5194/acp-15-13377-2015. [DOI] [Google Scholar]
  23. Xu L.; Guo H.; Boyd C. M.; Klein M.; Bougiatioti A.; Cerully K. M.; Hite J. R.; Isaacman-VanWertz G.; Kreisberg N. M.; Knote C.; Olson K.; Koss A.; Goldstein A. H.; Hering S. V.; de Gouw J.; Baumann K.; Lee S.-H.; Nenes A.; Weber R. J.; Ng N. L. Effects of anthropogenic emissions on aerosol formation from isoprene and monoterpenes in the southeastern United States. Proc. Natl. Acad. Sci. U. S. A. 2015, 112 (1), 37–42. 10.1073/pnas.1417609112. [DOI] [PMC free article] [PubMed] [Google Scholar]
  24. Fry J. L.; Draper D. C.; Zarzana K. J.; Campuzano-Jost P.; Day D. A.; Jimenez J. L.; Brown S. S.; Cohen R. C.; Kaser L.; Hansel A.; Cappellin L.; Karl T.; Hodzic Roux A.; Turnipseed A.; Cantrell C.; Lefer B. L.; Grossberg N. Observations of gas- and aerosol-phase organic nitrates at BEACHON-RoMBAS 2011. Atmos. Chem. Phys. 2013, 13 (17), 8585–8605. 10.5194/acp-13-8585-2013. [DOI] [Google Scholar]
  25. Rollins A. W.; Browne E. C.; Min K. E.; Pusede S. E.; Wooldridge P. J.; Gentner D. R.; Goldstein A. H.; Liu S.; Day D. A.; Russell L. M.; Cohen R. C. Evidence for NOx Control over Nighttime SOA Formation. Science 2012, 337 (6099), 1210–1212. 10.1126/science.1221520. [DOI] [PubMed] [Google Scholar]
  26. Massoli P.; Stark H.; Canagaratna M. R.; Krechmer J. E.; Xu L.; Ng N. L.; Mauldin R. L.; Yan C.; Kimmel J.; Misztal P. K.; Jimenez J. L.; Jayne J. T.; Worsnop D. R. Ambient Measurements of Highly Oxidized Gas-Phase Molecules during the Southern Oxidant and Aerosol Study (SOAS) 2013. ACS Earth Space Chem. 2018, 2 (7), 653–672. 10.1021/acsearthspacechem.8b00028. [DOI] [Google Scholar]
  27. Moise T.; Flores J. M.; Rudich Y. Optical Properties of Secondary Organic Aerosols and Their Changes by Chemical Processes. Chem. Rev. 2015, 115 (10), 4400–4439. 10.1021/cr5005259. [DOI] [PubMed] [Google Scholar]
  28. Flores J. M.; Zhao D. F.; Segev L.; Schlag P.; Kiendler-Scharr A.; Fuchs H.; Watne A. K.; Bluvshtein N.; Mentel T. F.; Hallquist M.; Rudich Y. Evolution of the complex refractive index in the UV spectral region in ageing secondary organic aerosol. Atmos. Chem. Phys. 2014, 14 (11), 5793–5806. 10.5194/acp-14-5793-2014. [DOI] [Google Scholar]
  29. Kim H.; Barkey B.; Paulson S. E. Real refractive indices of α- and β-pinene and toluene secondary organic aerosols generated from ozonolysis and photo-oxidation. J. Geophys. Res. Atmos. 2010, 115 (D24), D24212. 10.1029/2010JD014549. [DOI] [Google Scholar]
  30. Nakayama T.; Sato K.; Matsumi Y.; Imamura T.; Yamazaki A.; Uchiyama A. Wavelength Dependence of Refractive Index of Secondary Organic Aerosols Generated during the Ozonolysis and Photooxidation of alpha-Pinene. Sola 2012, 8, 119–123. 10.2151/sola.2012-030. [DOI] [Google Scholar]
  31. Liu P. F.; Zhang Y.; Martin S. T. Complex Refractive Indices of Thin Films of Secondary Organic Materials by Spectroscopic Ellipsometry from 220 to 1200 nm. Environ. Sci. Technol. 2013, 47 (23), 13594–13601. 10.1021/es403411e. [DOI] [PubMed] [Google Scholar]
  32. Lambe A. T.; Cappa C. D.; Massoli P.; Onasch T. B.; Forestieri S. D.; Martin A. T.; Cummings M. J.; Croasdale D. R.; Brune W. H.; Worsnop D. R.; Davidovits P. Relationship between Oxidation Level and Optical Properties of Secondary Organic Aerosol. Environ. Sci. Technol. 2013, 47 (12), 6349–6357. 10.1021/es401043j. [DOI] [PubMed] [Google Scholar]
  33. He Q.; Bluvshtein N.; Segev L.; Meidan D.; Flores J. M.; Brown S. S.; Brune W.; Rudich Y. Evolution of the Complex Refractive Index of Secondary Organic Aerosols during Atmospheric Aging. Environ. Sci. Technol. 2018, 52 (6), 3456–3465. 10.1021/acs.est.7b05742. [DOI] [PubMed] [Google Scholar]
  34. Nakayama T.; Sato K.; Imamura T.; Matsumi Y. Effect of Oxidation Process on Complex Refractive Index of Secondary Organic Aerosol Generated from Isoprene. Environ. Sci. Technol. 2018, 52 (5), 2566–2574. 10.1021/acs.est.7b05852. [DOI] [PubMed] [Google Scholar]
  35. Peng C.; Wang W.; Li K.; Li J.; Zhou L.; Wang L.; Ge M. The Optical Properties of Limonene Secondary Organic Aerosols: The Role of NO3, OH, and O3 in the Oxidation Processes. J. Geophys. Res.: Atmos. 2018, 123 (6), 3292–3303. 10.1002/2017JD028090. [DOI] [Google Scholar]
  36. Song C.; Gyawali M.; Zaveri R. A.; Shilling J. E.; Arnott W. P. Light absorption by secondary organic aerosol from α-pinene: Effects of oxidants, seed aerosol acidity, and relative humidity. J. Geophys. Res. Atmos. 2013, 118 (20), 11741–11749. 10.1002/jgrd.50767. [DOI] [Google Scholar]
  37. Varma R. M.; Ball S. M.; Brauers T.; Dorn H. P.; Heitmann U.; Jones R. L.; Platt U.; Pöhler D.; Ruth A. A.; Shillings A. J. L.; Thieser J.; Wahner A.; Venables D. S. Light extinction by secondary organic aerosol: an intercomparison of three broadband cavity spectrometers. Atmos. Meas. Tech. 2013, 6 (11), 3115–3130. 10.5194/amt-6-3115-2013. [DOI] [Google Scholar]
  38. Washenfelder R. A.; Attwood A. R.; Brock C. A.; Guo H.; Xu L.; Weber R. J.; Ng N. L.; Allen H. M.; Ayres B. R.; Baumann K.; Cohen R. C.; Draper D. C.; Duffey K. C.; Edgerton E.; Fry J. L.; Hu W. W.; Jimenez J. L.; Palm B. B.; Romer P.; Stone E. A.; Wooldridge P. J.; Brown S. S. Biomass burning dominates brown carbon absorption in the rural southeastern United States. Geophys. Res. Lett. 2015, 42 (2), 653–664. 10.1002/2014GL062444. [DOI] [Google Scholar]
  39. Suarez-Bertoa R.; Picquet-Varrault B.; Tamas W.; Pangui E.; Doussin J. F. Atmospheric Fate of a Series of Carbonyl Nitrates: Photolysis Frequencies and OH-Oxidation Rate Constants. Environ. Sci. Technol. 2012, 46 (22), 12502–12509. 10.1021/es302613x. [DOI] [PubMed] [Google Scholar]
  40. Müller J. F.; Peeters J.; Stavrakou T. Fast photolysis of carbonyl nitrates from isoprene. Atmos. Chem. Phys. 2014, 14 (5), 2497–2508. 10.5194/acp-14-2497-2014. [DOI] [Google Scholar]
  41. Atkinson R. Gas-Phase Tropospheric Chemistry of Volatile Organic Compounds: 1. Alkanes and Alkenes. J. Phys. Chem. Ref. Data 1997, 26 (2), 215–290. 10.1063/1.556012. [DOI] [Google Scholar]
  42. Kolb C. E.; Cox R. A.; Abbatt J. P. D.; Ammann M.; Davis E. J.; Donaldson D. J.; Garrett B. C.; George C.; Griffiths P. T.; Hanson D. R.; Kulmala M.; McFiggans G.; Poschl U.; Riipinen I.; Rossi M. J.; Rudich Y.; Wagner P. E.; Winkler P. M.; Worsnop D. R.; O’Dowd C. D. An overview of current issues in the uptake of atmospheric trace gases by aerosols and clouds. Atmos. Chem. Phys. 2010, 10 (21), 10561–10605. 10.5194/acp-10-10561-2010. [DOI] [Google Scholar]
  43. Gross S.; Iannone R.; Xiao S.; Bertram A. K. Reactive uptake studies of NO3 and N2O5 on alkenoic acid, alkanoate, and polyalcohol substrates to probe nighttime aerosol chemistry. Phys. Chem. Chem. Phys. 2009, 11 (36), 7792–7803. 10.1039/b904741g. [DOI] [PubMed] [Google Scholar]
  44. Decker Z.; Zarzana K.; Coggon M. M.; Min K.-E.; Pollack I.; Ryerson T. B.; Peischl J.; Edwards P.; Dubé W. P.; Markovic M. Z.; et al. Nighttime chemical transformation in biomass burning plumes: a box model analysis initialized with aircraft observations. Environ. Sci. Technol. 2019, 53, 2529–2538. 10.1021/acs.est.8b05359. [DOI] [PubMed] [Google Scholar]
  45. Baidar S.; Oetjen H.; Coburn S.; Dix B.; Ortega I.; Sinreich R.; Volkamer R. The CU Airborne MAX-DOAS instrument: vertical profiling of aerosol extinction and trace gases. Atmos. Meas. Tech. 2013, 6 (3), 719–739. 10.5194/amt-6-719-2013. [DOI] [Google Scholar]
  46. Aiken A. C.; DeCarlo P. F.; Jimenez J. L. Elemental analysis of organic species with electron ionization high-resolution mass spectrometry. Anal. Chem. 2007, 79 (21), 8350–8358. 10.1021/ac071150w. [DOI] [PubMed] [Google Scholar]
  47. Canagaratna M. R.; Jimenez J. L.; Kroll J. H.; Chen Q.; Kessler S. H.; Massoli P.; Hildebrandt Ruiz L.; Fortner E.; Williams L. R.; Wilson K. R.; Surratt J. D.; Donahue N. M.; Jayne J. T.; Worsnop D. R. Elemental ratio measurements of organic compounds using aerosol mass spectrometry: characterization, improved calibration, and implications. Atmos. Chem. Phys. 2015, 15 (1), 253–272. 10.5194/acp-15-253-2015. [DOI] [Google Scholar]
  48. Harrison M. A. J.; Barra S.; Borghesi D.; Vione D.; Arsene C.; Iulian Olariu R. Nitrated phenols in the atmosphere: a review. Atmos. Environ. 2005, 39 (2), 231–248. 10.1016/j.atmosenv.2004.09.044. [DOI] [Google Scholar]
  49. Bluvshtein N.; Flores J. M.; Segev L.; Rudich Y. A new approach for retrieving the UV–vis optical properties of ambient aerosols. Atmos. Meas. Tech. 2016, 9 (8), 3477–3490. 10.5194/amt-9-3477-2016. [DOI] [Google Scholar]
  50. Washenfelder R. A.; Attwood A. R.; Flores J. M.; Zarzana K. J.; Rudich Y.; Brown S. S. Broadband cavity-enhanced absorption spectroscopy in the ultraviolet spectral region for measurements of nitrogen dioxide and formaldehyde. Atmos. Meas. Tech. 2016, 9 (1), 41–52. 10.5194/amt-9-41-2016. [DOI] [Google Scholar]
  51. Flores J. M.; Washenfelder R. A.; Adler G.; Lee H. J.; Segev L.; Laskin J.; Laskin A.; Nizkorodov S. A.; Brown S. S.; Rudich Y. Complex refractive indices in the near-ultraviolet spectral region of biogenic secondary organic aerosol aged with ammonia. Phys. Chem. Chem. Phys. 2014, 16 (22), 10629–10642. 10.1039/C4CP01009D. [DOI] [PubMed] [Google Scholar]
  52. Washenfelder R. A.; Flores J. M.; Brock C. A.; Brown S. S.; Rudich Y. Broadband measurements of aerosol extinction in the ultraviolet spectral region. Atmos. Meas. Tech. 2013, 6 (4), 861–877. 10.5194/amt-6-861-2013. [DOI] [Google Scholar]
  53. Michel Flores J.; Bar-Or R. Z.; Bluvshtein N.; Abo-Riziq A.; Kostinski A.; Borrmann S.; Koren I.; Koren I.; Rudich Y. Absorbing aerosols at high relative humidity: linking hygroscopic growth to optical properties. Atmos. Chem. Phys. 2012, 12 (12), 5511–5521. 10.5194/acp-12-5511-2012. [DOI] [Google Scholar]
  54. Lang-Yona N.; Rudich Y.; Segre E.; Dinar E.; Abo-Riziq A. Complex Refractive Indices of Aerosols Retrieved by Continuous Wave-Cavity Ring Down Aerosol Spectrometer. Anal. Chem. 2009, 81 (5), 1762–1769. 10.1021/ac8017789. [DOI] [PubMed] [Google Scholar]
  55. Abo Riziq A.; Erlick C.; Dinar E.; Rudich Y. Optical properties of absorbing and non-absorbing aerosols retrieved by cavity ring down (CRD) spectroscopy. Atmos. Chem. Phys. 2007, 7 (6), 1523–1536. 10.5194/acp-7-1523-2007. [DOI] [Google Scholar]
  56. Yeh G. K.; Claflin M. S.; Ziemann P. J. Products and Mechanism of the Reaction of 1-Pentadecene with NO3 Radicals and the Effect of a – ONO2 Group on Alkoxy Radical Decomposition. J. Phys. Chem. A 2015, 119 (43), 10684–10696. 10.1021/acs.jpca.5b07468. [DOI] [PubMed] [Google Scholar]
  57. Claflin M. S.; Ziemann P. J. Identification and Quantitation of Aerosol Products of the Reaction of β-Pinene with NO3 Radicals and Implications for Gas- and Particle-Phase Reaction Mechanisms. J. Phys. Chem. A 2018, 122 (14), 3640–3652. 10.1021/acs.jpca.8b00692. [DOI] [PubMed] [Google Scholar]
  58. Bianchi F.; Kurtén T.; Riva M.; Mohr C.; Rissanen M. P.; Roldin P.; Berndt T.; Crounse J. D.; Wennberg P. O.; Mentel T. F.; Wildt J.; Junninen H.; Jokinen T.; Kulmala M.; Worsnop D. R.; Thornton J. A.; Donahue N.; Kjaergaard H. G.; Ehn M. Highly Oxygenated Organic Molecules (HOM) from Gas-Phase Autoxidation Involving Peroxy Radicals: A Key Contributor to Atmospheric Aerosol. Chem. Rev. 2019, 119 (6), 3472–3509. 10.1021/acs.chemrev.8b00395. [DOI] [PMC free article] [PubMed] [Google Scholar]
  59. Ehn M.; Thornton J. A.; Kleist E.; Sipila M.; Junninen H.; Pullinen I.; Springer M.; Rubach F.; Tillmann R.; Lee B.; Lopez-Hilfiker F.; Andres S.; Acir I. H.; Rissanen M.; Jokinen T.; Schobesberger S.; Kangasluoma J.; Kontkanen J.; Nieminen T.; Kurten T.; Nielsen L. B.; Jorgensen S.; Kjaergaard H. G.; Canagaratna M.; Maso M. D.; Berndt T.; Petaja T.; Wahner A.; Kerminen V. M.; Kulmala M.; Worsnop D. R.; Wildt J.; Mentel T. F. A large source of low-volatility secondary organic aerosol. Nature 2014, 506 (7489), 476–9. 10.1038/nature13032. [DOI] [PubMed] [Google Scholar]
  60. Mentel T. F.; Springer M.; Ehn M.; Kleist E.; Pullinen I.; Kurtén T.; Rissanen M.; Wahner A.; Wildt J. Formation of highly oxidized multifunctional compounds: autoxidation of peroxy radicals formed in the ozonolysis of alkenes – deduced from structure–product relationships. Atmos. Chem. Phys. 2015, 15 (12), 6745–6765. 10.5194/acp-15-6745-2015. [DOI] [Google Scholar]
  61. Berndt T.; Richters S.; Jokinen T.; Hyttinen N.; Kurten T.; Otkjaer R. V.; Kjaergaard H. G.; Stratmann F.; Herrmann H.; Sipila M.; Kulmala M.; Ehn M. Hydroxyl radical-induced formation of highly oxidized organic compounds. Nat. Commun. 2016, 7, 13677. 10.1038/ncomms13677. [DOI] [PMC free article] [PubMed] [Google Scholar]
  62. Berndt T.; Scholz W.; Mentler B.; Fischer L.; Herrmann H.; Kulmala M.; Hansel A. Accretion Product Formation from Self- and Cross-Reactions of RO2 Radicals in the Atmosphere. Angew. Chem., Int. Ed. 2018, 57 (14), 3820–3824. 10.1002/anie.201710989. [DOI] [PubMed] [Google Scholar]
  63. Berndt T.; Mentler B.; Scholz W.; Fischer L.; Herrmann H.; Kulmala M.; Hansel A. Accretion Product Formation from Ozonolysis and OH Radical Reaction of alpha-Pinene: Mechanistic Insight and the Influence of Isoprene and Ethylene. Environ. Sci. Technol. 2018, 52 (19), 11069–11077. 10.1021/acs.est.8b02210. [DOI] [PubMed] [Google Scholar]
  64. 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.; Prevot A. S. H.; Dinar E.; Rudich Y.; Worsnop D. R. Organic aerosol components observed in Northern Hemispheric datasets from Aerosol Mass Spectrometry. Atmos. Chem. Phys. 2010, 10 (10), 4625–4641. 10.5194/acp-10-4625-2010. [DOI] [Google Scholar]
  65. Ng N. L.; Canagaratna M. R.; Jimenez J. L.; Zhang Q.; Ulbrich I. M.; Worsnop D. R. Real-Time Methods for Estimating Organic Component Mass Concentrations from Aerosol Mass Spectrometer Data. Environ. Sci. Technol. 2011, 45 (3), 910–916. 10.1021/es102951k. [DOI] [PubMed] [Google Scholar]
  66. Hu W.; Campuzano-Jost P.; Day D. A.; Croteau P.; Canagaratna M. R.; Jayne J. T.; Worsnop D. R.; Jimenez J. L. Evaluation of the new capture vaporizer for Aerosol Mass Spectrometers (AMS) through laboratory studies of inorganic species. Atmos. Meas. Tech. 2017, 10 (8), 2897–2921. 10.5194/amt-10-2897-2017. [DOI] [Google Scholar]
  67. Struckmeier C.; Drewnick F.; Fachinger F.; Gobbi G. P.; Borrmann S. Atmospheric aerosols in Rome, Italy: sources, dynamics and spatial variations during two seasons. Atmos. Chem. Phys. 2016, 16 (23), 15277–15299. 10.5194/acp-16-15277-2016. [DOI] [Google Scholar]
  68. Farmer D. K.; Matsunaga A.; Docherty K. S.; Surratt J. D.; Seinfeld J. H.; Ziemann P. J.; Jimenez J. L. Response of an aerosol mass spectrometer to organonitrates and organosulfates and implications for atmospheric chemistry. Proc. Natl. Acad. Sci. U. S. A. 2010, 107 (15), 6670–6675. 10.1073/pnas.0912340107. [DOI] [PMC free article] [PubMed] [Google Scholar]
  69. Xu L.; Suresh S.; Guo H.; Weber R. J.; Ng N. L. Aerosol characterization over the southeastern United States using high-resolution aerosol mass spectrometry: spatial and seasonal variation of aerosol composition and sources with a focus on organic nitrates. Atmos. Chem. Phys. 2015, 15 (13), 7307–7336. 10.5194/acp-15-7307-2015. [DOI] [Google Scholar]
  70. Bruns E. A.; Perraud V.; Zelenyuk A.; Ezell M. J.; Johnson S. N.; Yu Y.; Imre D.; Finlayson-Pitts B. J.; Alexander M. L. Comparison of FTIR and Particle Mass Spectrometry for the Measurement of Particulate Organic Nitrates. Environ. Sci. Technol. 2010, 44 (3), 1056–1061. 10.1021/es9029864. [DOI] [PubMed] [Google Scholar]
  71. Fry J. L.; Kiendler-Scharr A.; Rollins A. W.; Brauers T.; Brown S. S.; Dorn H. P.; Dubé W. P.; Fuchs H.; Mensah A.; Rohrer F.; Tillmann R.; Wahner A.; Wooldridge P. J.; Cohen R. C. SOA from limonene: role of NO3 in its generation and degradation. Atmos. Chem. Phys. 2011, 11 (8), 3879–3894. 10.5194/acp-11-3879-2011. [DOI] [Google Scholar]
  72. Fry J. L.; Kiendler-Scharr A.; Rollins A. W.; Wooldridge P. J.; Brown S. S.; Fuchs H.; Dubé W.; Mensah A.; dal Maso M.; Tillmann R.; Dorn H. P.; Brauers T.; Cohen R. C. Organic nitrate and secondary organic aerosol yield from NO3 oxidation of β-pinene evaluated using a gas-phase kinetics/aerosol partitioning model. Atmos. Chem. Phys. 2009, 9 (4), 1431–1449. 10.5194/acp-9-1431-2009. [DOI] [Google Scholar]
  73. Rollins A. W.; Kiendler-Scharr A.; Fry J. L.; Brauers T.; Brown S. S.; Dorn H. P.; Dubé W. P.; Fuchs H.; Mensah A.; Mentel T. F.; Rohrer F.; Tillmann R.; Wegener R.; Wooldridge P. J.; Cohen R. C. Isoprene oxidation by nitrate radical: alkyl nitrate and secondary organic aerosol yields. Atmos. Chem. Phys. 2009, 9 (18), 6685–6703. 10.5194/acp-9-6685-2009. [DOI] [Google Scholar]
  74. Boyd C. M.; Sanchez J.; Xu L.; Eugene A. J.; Nah T.; Tuet W. Y.; Guzman M. I.; Ng N. L. Secondary organic aerosol formation from the β-pinene+NO3 system: effect of humidity and peroxy radical fate. Atmos. Chem. Phys. 2015, 15 (13), 7497–7522. 10.5194/acp-15-7497-2015. [DOI] [Google Scholar]
  75. Boyd C. M.; Nah T.; Xu L.; Berkemeier T.; Ng N. L. Secondary Organic Aerosol (SOA) from Nitrate Radical Oxidation of Monoterpenes: Effects of Temperature, Dilution, and Humidity on Aerosol Formation, Mixing, and Evaporation. Environ. Sci. Technol. 2017, 51 (14), 7831–7841. 10.1021/acs.est.7b01460. [DOI] [PubMed] [Google Scholar]
  76. Liu P. F.; Abdelmalki N.; Hung H. M.; Wang Y.; Brune W. H.; Martin S. T. Ultraviolet and visible complex refractive indices of secondary organic material produced by photooxidation of the aromatic compounds toluene and m-xylene. Atmos. Chem. Phys. 2015, 15 (3), 1435–1446. 10.5194/acp-15-1435-2015. [DOI] [Google Scholar]
  77. Saleh R.; Hennigan C. J.; McMeeking G. R.; Chuang W. K.; Robinson E. S.; Coe H.; Donahue N. M.; Robinson A. L. Absorptivity of brown carbon in fresh and photo-chemically aged biomass-burning emissions. Atmos. Chem. Phys. 2013, 13 (15), 7683–7693. 10.5194/acp-13-7683-2013. [DOI] [Google Scholar]
  78. Sumlin B. J.; Pandey A.; Walker M. J.; Pattison R. S.; Williams B. J.; Chakrabarty R. K. Atmospheric Photooxidation Diminishes Light Absorption by Primary Brown Carbon Aerosol from Biomass Burning. Environ. Sci. Technol. Lett. 2017, 4 (12), 540–545. 10.1021/acs.estlett.7b00393. [DOI] [Google Scholar]
  79. Li C.; He Q.; Schade J.; Passig J.; Zimmermann R.; Meidan D.; Laskin A.; Rudich Y. Dynamic changes in optical and chemical properties of tar ball aerosols by atmospheric photochemical aging. Atmos. Chem. Phys. 2019, 19 (1), 139–163. 10.5194/acp-19-139-2019. [DOI] [Google Scholar]
  80. Bluvshtein N.; Lin P.; Flores J. M.; Segev L.; Mazar Y.; Tas E.; Snider G.; Weagle C.; Brown S. S.; Laskin A.; Rudich Y. Broadband optical properties of biomass-burning aerosol and identification of brown carbon chromophores. J. Geophys. Res. Atmos. 2017, 122 (10), 5441–5456. 10.1002/2016JD026230. [DOI] [Google Scholar]
  81. Jiang H. H.; Frie A. L.; Lavi A.; Chen J. Y.; Zhang H. F.; Bahreini R.; Lin Y. H. Brown Carbon Formation from Nighttime Chemistry of Unsaturated Heterocyclic Volatile Organic Compounds. Environ. Sci. Technol. Lett. 2019, 6 (3), 184–190. 10.1021/acs.estlett.9b00017. [DOI] [Google Scholar]
  82. Nakayama T.; Sato K.; Matsumi Y.; Imamura T.; Yamazaki A.; Uchiyama A. Wavelength and NOx dependent complex refractive index of SOAs generated from the photooxidation of toluene. Atmos. Chem. Phys. 2013, 13 (2), 531–545. 10.5194/acp-13-531-2013. [DOI] [Google Scholar]
  83. Li C.; He Q.; Schade J.; Passig J.; Zimmermann R.; Meidan D.; Laskin A.; Rudich Y. Dynamic changes in optical and chemical properties of tar ball aerosols by atmospheric photochemical aging. Atmos. Chem. Phys. 2019, 19 (1), 139–163. 10.5194/acp-19-139-2019. [DOI] [Google Scholar]
  84. Tong H. J.; Arangio A. M.; Lakey P. S. J.; Berkemeier T.; Liu F. B.; Kampf C. J.; Brune W. H.; Poschl U.; Shiraiwa M. Hydroxyl radicals from secondary organic aerosol decomposition in water. Atmos. Chem. Phys. 2016, 16 (3), 1761–1771. 10.5194/acp-16-1761-2016. [DOI] [Google Scholar]
  85. Zhang X.; Zhang H.; Xu W.; Wu X.; Tyndall G. S.; Orlando J. J.; Jayne J. T.; Worsnop D. R.; Canagaratna M. R. Molecular characterization of alkyl nitrates in atmospheric aerosols by ion mobility mass spectrometry. Atmos. Meas. Tech. 2019, 12 (10), 5535–5545. 10.5194/amt-12-5535-2019. [DOI] [Google Scholar]
  86. Redmond H.; Thompson J. E. Evaluation of a quantitative structure-property relationship (QSPR) for predicting mid-visible refractive index of secondary organic aerosol (SOA). Phys. Chem. Chem. Phys. 2011, 13 (15), 6872–6882. 10.1039/c0cp02270e. [DOI] [PubMed] [Google Scholar]
  87. Bosque R.; Sales J. Polarizabilities of Solvents from the Chemical Composition. J. Chem. Inf. Comput. Sci. 2002, 42 (5), 1154–1163. 10.1021/ci025528x. [DOI] [PubMed] [Google Scholar]
  88. Jacobson M. Z.; Kaufman Y. J.; Rudich Y. Examining feedbacks of aerosols to urban climate with a model that treats 3-D clouds with aerosol inclusions. J. Geophys. Res. 2007, 112 (D24), D24205. 10.1029/2007JD008922. [DOI] [Google Scholar]
  89. Saleh R. From Measurements to Models: Toward Accurate Representation of Brown Carbon in Climate Calculations. Curr. Pollut. Rep. 2020, 6 (2), 90–104. 10.1007/s40726-020-00139-3. [DOI] [Google Scholar]

Associated Data

This section collects any data citations, data availability statements, or supplementary materials included in this article.

Supplementary Materials

es0c06838_si_001.pdf (2.5MB, pdf)

Articles from Environmental Science & Technology are provided here courtesy of American Chemical Society

RESOURCES