Articles | Volume 23, issue 6
Research article
28 Mar 2023
Research article |  | 28 Mar 2023

A combined gas- and particle-phase analysis of highly oxygenated organic molecules (HOMs) from α-pinene ozonolysis

Jian Zhao, Ella Häkkinen, Frans Graeffe, Jordan E. Krechmer, Manjula R. Canagaratna, Douglas R. Worsnop, Juha Kangasluoma, and Mikael Ehn

Highly oxygenated organic molecules (HOMs) are important for the formation of secondary organic aerosol (SOA), which poses serious health risks and exerts great influence on Earth's climate. However, the speciation of particle-phase HOMs and its relationship with gas-phase HOM formation has been limited by the lack of suitable analytical techniques. Here, combining a novel particle evaporation inlet, the VIA (Vaporization Inlet for Aerosols), with a nitrate chemical ionization mass spectrometer (NO3-CIMS), gas- and particle-phase HOM products of α-pinene ozonolysis were studied under different conditions. Within the 50 min residence time of our Teflon chamber, we observed enhancement of C16C19 HOM dimers in particles compared to the HOMs that were condensing. In particular, gas-phase dimer formation was considerably suppressed in experiments with the addition of CO or NO, but dimers still made up a considerable fraction of the observed SOA. In addition to the generally shorter carbon skeletons of the particle-phase dimers (i.e., C16C19) compared to the gas phase (C19C20), average O/C ratios of the HOMs (especially in the dimer range) also decreased slightly in the particle phase. C17H26Oz compounds, which have often been reported by previous offline measurements, dominate the particle-phase HOM mass spectra in α-pinene ozonolysis experiments. Our results indicate that these C17 compounds might be related to particle-phase processes within 1 h after HOM condensation. However, the new VIA–NO3-CIMS system used in this work will require more detailed characterization to better understand how the thermal desorption and wall effects may modify the measured particle-phase HOM distributions. Nevertheless, organic nitrate, for example, measured by this novel VIA–NO3-CIMS system was consistent with the measurements of an Aerodyne aerosol mass spectrometer (AMS), showing the capability of this system as a promising technique for particle-phase HOM measurements. Taken together, we believe that this system is a promising technique for combined online gas- and particle-phase HOM measurements.

1 Introduction

Secondary organic aerosol (SOA), formed from condensable oxidation products of volatile organic compounds (VOCs), contributes a large fraction to tropospheric fine particles, which greatly influence human health and global climate (Mauderly and Chow, 2008; Jimenez et al., 2009; Boucher et al., 2013). Recently, highly oxygenated organic molecules (HOMs) formed through rapid autoxidation (i.e., consecutive intramolecular H shifts followed by O2 addition) of peroxy radicals (RO2) were found to play an important role in the growth and/or formation of new particles in the atmosphere (Crounse et al., 2013; Ehn et al., 2014; Kulmala et al., 2014; Jokinen et al., 2014; Kirkby et al., 2016; Bianchi et al., 2019). RO2 constitutes ubiquitous intermediates formed from the attack of various oxidants on VOC precursors, and therefore the fate of RO2 and related formation pathways toward HOMs is crucial to understanding the gas-phase chemistry and corresponding SOA formation in Earth's lower atmosphere (Orlando and Tyndall, 2012; Ehn et al., 2017).

Monoterpenes (C10H16), emitted from various terrestrial vegetation systems, account for ∼15 % of biogenic VOCs emissions (by mass) at a global scale (Guenther et al., 2012) and may contribute largely to fine organic aerosols (Ding et al., 2014; Zhang et al., 2018; McFiggans et al., 2019). α-pinene (AP) is one of the most important monoterpenes, which has been shown to form C10 monomers and C20 dimers as HOM products (Ehn et al., 2014). An endocyclic double bond and relatively large carbon skeleton increase the yield of these low-volatility HOM products compared to many other biogenic VOCs (e.g., isoprene C5H8, the most abundant biogenic gas precursor), making it important in terms of SOA formation (Donahue et al., 2012, 2013; Jokinen et al., 2015; Kurtén et al., 2016). Furthermore, the ozonolysis of α-pinene produces aldehydic H atoms, which greatly promotes H shifts in the RO2 and consequently increases HOM yields (Mentel et al., 2015; Rissanen et al., 2014; Bianchi et al., 2019). Consistently, HOM yields from other oxidants (e.g., OH, NO3, and Cl) reacting with α-pinene are typically lower (Jokinen et al., 2015; Berndt et al., 2016; Kurtén et al., 2017; Wang et al., 2020). These recent HOM yield findings are also consistent with earlier SOA mass yields, which have shown that O3 forms more SOA than the other oxidants (Hoffmann et al., 1997; Griffin et al., 1999; Presto et al., 2005).

The understanding of HOM formation from ozonolysis of α-pinene has gradually improved during the past decade, owing to the developments and improvements of state-of-the-art mass spectrometers and quantum chemical calculations (Ehn et al., 2012; Vereecken et al., 2015; Riva et al., 2019; Bianchi et al., 2019; Iyer et al., 2021). The nitrate chemical ionization inlet combined with an atmospheric pressure interface time-of-flight mass spectrometer (NO3-CIMS for short hereafter) has been widely used to detect gas-phase HOMs as adduct clusters with NO3- with high sensitivity and selectivity (Junninen et al., 2010; Jokinen et al., 2012; Ehn et al., 2014; Hyttinen et al., 2017). Other reagent ions (e.g., CH3COO, C3H7NH3+, and NH4+) have also been used with different sensitivities and selectivities to increase our understanding of HOM species and autoxidation (Berndt et al., 2016, 2018; Riva et al., 2019). However, the characterization of HOMs in the particle phase as well as the physicochemical links between gas- and particle-phase HOMs are still not clear. One of the difficulties is the lack of suitable analytical techniques to identify the labile peroxides in α-pinene SOA (Docherty et al., 2005; Reinnig et al., 2009; Krapf et al., 2016), which are formed literally after each H shift of RO2 during HOM formation in the gas phase (Crounse et al., 2013; Mentel et al., 2015; Wang et al., 2017). The lifetime of organic peroxides in α-pinene SOA was reported to be around 1 h through dark decomposition (Krapf et al., 2016). Formation of high-molecular-weight ester dimers with aldehydes and ketones through the Baeyer–Villiger reactions was proposed as another particle-phase loss of these hydroperoxides (Claflin et al., 2018). The concomitant formation of carboxylic acids through the Baeyer–Villiger reactions is consistent with the fact that a large portion of organic acids was observed in ambient SOA (Hallquist et al., 2009; Yatavelli et al., 2015). However, the experiments conducted by Claflin et al. (2018) were under conditions of high VOC concentrations (corresponding to 3 mg m−3 SOA), and whether the proposed reactions can happen under ambient conditions is still unknown. Another study suggested that some HOM species (assumed to be keto-hydroperoxides) may undergo decomposition through the Korcek mechanism in the particle phase, which forms C7C9 carboxylic acids and C1C4 carbonyls (Mutzel et al., 2015).

Here, a novel particle evaporation inlet named the VIA (Vaporization Inlet for Aerosols, Aerodyne Research, Inc.), combined with an NO3-CIMS was, used to detect HOMs in the particle phase at trace concentrations. There are several special features of this system compared to currently used or developed techniques (Häkkinen et al., 2022). Traditional molecular-level SOA measurements are usually conducted in an offline or semi-online way, during which filters or metal surfaces are necessary to collect particles (Hallquist et al., 2009; Yatavelli et al., 2012; Mutzel et al., 2015). We tried to minimize unwanted surface reactions of SOA by heating it directly within the sampling flow after removing the gases, which is important for the detection of labile organic compounds. Another online technique that was recently developed is the extractive electrospray ionization (EESI) inlet combined with a mass spectrometer, aimed at providing rapid online molecular detection of SOA (Lopez-Hilfiker et al., 2019; Pospisilova et al., 2020) and updated to a dual-phase inlet by Lee et al. (2022). The EESI has proven very useful for SOA detection, but it cannot provide comparable gas-phase measurements. Both gas- and particle-phase organic molecules could be detected by the Filter Inlet for Gases and Aerosols (FIGAERO) coupled with an iodide or acetate CIMS (Lopez-Hilfiker et al., 2014, 2015) or a chemical analysis of aerosol online (CHARON) inlet coupled with a proton-transfer-reaction (PTR) mass spectrometer (Eichler et al., 2015; Müller et al., 2017). These are robust and powerful systems for online (CHARON) or semi-online (FIGAERO) SOA measurements, though each reagent ion and setup provides its own selectivity and sensitivity, with neither being specifically selective towards HOMs (Riva et al., 2019). Recently, a thermal desorption–differential mobility analyzer (TD-DMA) coupled with an NO3-CIMS was deployed to detect nano-SOA (∼10–30 nm) particles in a semi-online approach (Wagner et al., 2018; Caudillo et al., 2021). Similar to our system, nitrate was used as the reagent ion for both gas- and particle-phase measurements, reducing ambiguities when comparing HOM species measured in the gas versus particle phase. The advantage of the TD-DMA system is that it uses a DMA to size-select particles, but the drawback is the lowered (bulk) sensitivity due to the need for charging in the DMA. Thus, the novel VIA coupled with an NO3-CIMS will be a promising system to identify HOM species in the particle phase using a fully online approach.

In this work, in order to provide molecular speciation of HOMs in the particle phase and deduce their dependence on HOMs formed in the gas phase, we systematically studied HOM products in both phases using the novel VIA–NO3-CIMS system. From our earlier experiments, higher dimer than monomer concentrations were observed in the particle phase for four different VOCs using this system (Häkkinen et al., 2022), in contrast to the measurements in the gas phase. However, those experiments were mainly focused on the particle phase and were conducted with high precursor conditions using a potential aerosol mass (PAM) reactor (Kang et al., 2007; Lambe et al., 2011). Here, starting with relatively lower concentrations of α-pinene and O3 (dark reactions) as our base case in a Teflon chamber, CO or NO2/NO was introduced into this reaction system to change the distribution of HOM products and meanwhile investigate the impacts in both the gas and particle phases. HOM products were grouped according to different carbon numbers, along with dimer to monomer ratios (D/M), to compare their distribution in different phases. In addition, bulk chemical compositions (O/C, H/C, and N/C) of HOMs in the particle phase were estimated and compared to a widely used Aerodyne aerosol mass spectrometer (DeCarlo et al., 2006).

2 Experimental section

2.1 Experimental setup

The setup for experiments conducted in this work includes three parts as shown in Fig. 1. (a) The first is a reaction chamber (2 m3, Teflon), in which HOMs and SOA were formed from α-pinene ozonolysis. The experiments were operated in a continuous-flow mode (residence time ∼50 min) under dry conditions (RH < 2 %) and at room temperature (26±1,C). The total inflow of 40 L min−1 cleaned air was purified by a clean air generator (AADCO model 737-14, Ohio, USA). α-Pinene was injected using a syringe (Hamilton) and a syringe pump (Cole-Parmer, IL, USA). O3 was generated by an ozone generator (Dasibi 1008-PC). Sodium chloride solution (NaCl in Milli-Q water) was used to generate seed particles (80 nm) to make the HOMs condense onto larger particles rather than forming new (small) particles. NaCl was used instead of the more common ammonium sulfate (AS) to prevent the potential depletion of reagent ions by large amounts of sulfuric acid and to avoid its nucleation with evaporated HOM vapors. CO or NO2 was injected into the chamber from a gas cylinder during some of the experiments to change the gas-phase HOM chemistry. NO was generated from photolysis of NO2 with UV lights (400 nm, The entire flow system was controlled by a series of mass-flow controllers (MKS, G-series, 0.05–50 L min−1, Andover, MA, USA). For more detailed descriptions of the “COALA” chamber system and facilities at the University of Helsinki, please refer to Riva et al. (2019) and Peräkylä et al. (2020).

Figure 1Setup for the thermal evaporation experiments used in this work. Note that all three parts (a–c) are necessary for the particle-phase HOM measurements, whereas only the parts in panels (a) and (c) are used for the gas-phase HOM measurements (i.e., all instruments sampling directly from the chamber).


(b) The second part is an SOA evaporation system; a novel VIA was deployed to evaporate particles for analysis. First, the gaseous vapors were removed from the sample flow (1.5–2 L min−1) by a honeycomb-activated charcoal denuder (shaded region in Fig. 1, panel b) in front of the heating region within the VIA. The remaining particles were then heated to a chosen temperature (25 to 300 C, measured from the surface of the heating tube by a thermocouple), causing evaporation of molecules in the particles. After the VIA, a dilution flow (10 L min−1) was introduced, in part to cool down the sample before entering the NO3-CIMS and to provide enough flow for all instruments.

Table 1Experimental conditions for the COALA chamber experiments. The steady-state conditions refer to the stabilized concentrations before adding seed particles.

Download Print Version | Download XLSX

Based on our tests, the removal efficiency of this charcoal denuder depends on the flow rate through the VIA as well as the concentrations and types of target gas. The best removal performance was obtained with a small flow rate (1–2 L min−1). We observed that >95 % of ∼4 ppm O3 and >80 % of 500–800 ppb α-pinene were removed at 1.5 L min−1. Thus, the gas denuder worked efficiently under low concentrations used in this work (Table 1), and gas-phase reactions within the VIA were assumed to be negligible. The particle transmission efficiency of the VIA was ∼90 % tested with room air (10–200 nm particles). The denuder was replaced with a new or cleaned one before the start of each experiment to prevent potential contaminations, and it can be regenerated by heating to 100 C in a clean airflow for about 4 h. Using valves, we could either pass the sampled air through a high-efficiency particulate air (HEPA) filter to remove particles and through the VIA to remove the gaseous vapors for a background measurement, or we could bypass the HEPA and VIA completely to measure the unperturbed sample. However, to avoid the additional losses and dilution, direct gas-phase HOM measurements were done by completely bypassing the second part (b) of the setup. A more detailed characterization of this VIA–NO3-CIMS system was investigated in a previous work (Häkkinen et al., 2022).

Figure 2Overview of experiment no. 1 (input flow with 53 ppb α-pinene and 33 ppb O3). (a) Particle number concentration and size distribution sampled by SMPS as a function of time. Time series of (b) measured and modeled ozone and α-pinene concentration (1 min averaged) in the chamber; (c) gas-phase (solid lines, normalized to reagent ions at first and then to their maximums) and particle-phase (dashed lines, normalized to reagent ions) HOM species (10 s averaged); (d) total aerosol, organics, and sodium chloride mass concentrations from SMPS (2.2 min averaged, black circles) and AMS measurements (20 s averaged). The first and second shaded areas are gas-phase and particle-phase background measurements, respectively. Note that the time series of NaCl was estimated using the method explained in the Supplement owing to the lack of measurements, and no measurements given above were corrected for chamber wall loss.


(c) The third part involves measurements for which a suite of gas- and particle-phase instruments were deployed. Gas-phase and evaporated HOMs from SOA were measured by an NO3-CIMS (Tofwerk AG/Aerodyne Research, Inc.), which is highly sensitive to detect HOMs as adduct clusters with NO3- (Junninen et al., 2010; Jokinen et al., 2012). The NO3-CIMS was equipped with an Eisele inlet (Eisele and Tanner, 1993) and a long time-of-flight mass spectrometer, providing a mass resolution of ∼8500 above 125 Th. Nitrate ions were generated from nitric acid (HNO3) through an X-ray source. The concentrations of HOMs were estimated by applying a calibration factor Cx (=2×1010 cm−3) to the raw signals after being normalized by the sum of reagent ions (i.e., nitrate monomer, dimer, and trimer). This calibration factor was estimated using the sulfuric acid signals obtained by the VIA–NO3-CIMS system from several nanograms of AS assuming 70 % evaporation at 300 C (Häkkinen et al., 2022). Thus, a large uncertainty comes with this estimation, along with other factors including the total losses of HOMs during evaporation and sampling. We expect the uncertainty to be at least a factor of 3 (+200 % to −67 %), and therefore the absolute concentrations are only reported in this work to give rough approximations of the sampled concentrations. SOA mass was measured by a long time-of-flight aerosol mass spectrometer (LToF-AMS, Aerodyne Research, Inc.) using thermal evaporation (600 C) and electron impact ionization (70 eV) techniques (DeCarlo et al., 2006; Canagaratna et al., 2007). The (relative) ionization efficiency of AMS towards inorganic species was calibrated with 300 nm ammonium nitrate (AN) and AS particles (Jayne et al., 2000). The particle size distribution (10–500 nm) was measured with a scanning mobility particle sizer system (SMPS, consisting of one 3081 long differential mobility analyzer and one 3750 condensation particle counter, TSI). O3, NO, and NO2 were monitored by a UV photometric analyzer (model 49P, Thermo Environmental Instruments), an Eco Physics gas analyzer (model CLD 780 TR), and a chemiluminescence NO–NO2NOx analyzer (model 42i, Thermo Fisher Scientific), respectively. In addition, a proton transfer reaction time-of-flight mass spectrometer (PTR-ToF 8000, Ionicon Analytik GmbH) was used to measure α-pinene. Unfortunately, it worked intermittently and was only connected to the chamber twice during the first experiments. The concentrations of α-pinene in the first experiment were evaluated based on 5 min averaged signals from the data acquisition panel by applying the sensitivity obtained from the calibration conducted that morning (two brown cross markers in Fig. 2b). For the rest of the experiments, we used the syringe pump injection rates to estimate the injected concentrations of α-pinene.

2.2 Chamber experiments

A typical experiment was conducted as shown in Fig. 2, including two stages. In stage I, all instruments sampled directly from the chamber (i.e., the part in panel b in Fig. 1 was removed from the system). The COALA chamber was flushed with purified air for at least 12 h before each experiment (chamber background was determined during this period, first shaded area in Fig. 2). HOMs formed rapidly once α-pinene and O3 were injected into the chamber. SOA particles took ∼40 min to form and grow larger than 10 nm to be measured by an SMPS, whereas it took about 1.5 h for the AMS to capture the SOA formation. Then, NaCl seed particles were added into the chamber after HOM and SOA concentrations stabilized, which can be seen as a dramatic increase in the particle mass in Fig. 2d. However, the thermal desorption temperature of 600 C used by the AMS was not enough for effective NaCl evaporation or measurements, resulting in discrepancies in aerosol mass concentration compared to the SMPS (Fig. S1 in the Supplement). The mass concentrations shown in Fig. 2d were modified based on AMS and SMPS measurements, and the method to reconstruct SOA and NaCl mass is explained in the Supplement (Sect. S1). In contrast to the aerosol mass, gas-phase HOMs decreased upon seed addition owing to enhanced condensation onto the newly added particles that increased the condensation sink. By calculating the difference in gas-phase HOM spectra before and after seed particle addition, we can deduce the condensing HOM products. We will use the term “condensed gas phase” hereafter to directly compare the condensing HOMs to the particle-phase HOM measurements. In stage II, the VIA was mounted manually between the chamber and instruments for particle-phase HOM measurements as shown in Fig. 1. After background measurements for the particle phase (second shaded area in Fig. 2), three different temperatures (170, 230, and 300 C) were set for the VIA heater, each one kept for about 1 h for data collection. Note that the analysis and following discussions mainly focus on the results of 230 C, which was found to give the highest sensitivity and signals for total particle-phase HOM measurements with fewer losses or less thermal decomposition compared to other temperatures. However, as shown in Fig. 2c, larger molecules (C17 and C20 compounds) were found to evaporate more efficiently at 230 C than other temperatures, while signals of more volatile molecules (e.g., C10 compounds) were already decreasing at this temperature. This effect, whereby the choice of evaporation temperature significantly impacts the distribution of observed species, is consistent with the previous results reported by Häkkinen et al. (2022) and needs to be kept in mind when interpreting the particle-phase HOM mass spectra. Between the change in temperatures, the sampling line bypassed the VIA to obtain SOA mass concentration without heating. Then, the evaporated SOA mass could be estimated by taking the difference of measurements between bypass and VIA modes. At the end of the experiment, a test stage was included for determining kinetic parameters for use in a box model (described in Sect. 2.4), such as the flush-out rate (as shown in Fig. 2b) and the photolysis rate of NO2. All experiments conducted in this work are summarized in Table 1 and will be explained in Sect. 2.4.

2.3 Data analysis

The mass spectrometry datasets were analyzed using packages based on Igor Pro (WaveMetrics, Inc., USA) (Tofware_3_2_0 and ToF_AMS_HRAnalysis_v1_25A). Based on the mechanisms of HOM formation, “HOM” was suggested by Bianchi et al. (2019) to describe compounds directly related to gas-phase autoxidation (Crounse et al., 2013) in atmospheric conditions and with at least six oxygen atoms so that they could be effectively detected by an NO3-CIMS as used in this work. Although organic compounds with O numbers less than six (e.g., norpinic acid C8H12O4 and pinic acid C9H14O4) were largely observed in both the gas and particle phase in α-pinene ozonolysis (Lopez-Hilfiker et al., 2015; Zhang et al., 2015), these compounds would not be regarded as HOMs, nor would they be effectively detected by an NO3-CIMS (Hyttinen et al., 2015, 2017). For experiments with NOx, measured HOM signals were separated into two groups as HOMCHO (CxHyOz compounds) and N-containing HOMON (CxHyN1–2Oz compounds) based on the number of N atoms in the fitted molecular formula excluding the reagent ion (NO3-). The peak positions located at odd or even nominal mass also helped to separate these compounds. Note that a relatively low contribution of nitrate-dimer-charged (HNO3NO3-) signals to the total signal (4.3±1.5 %) was observed for α-pinene ozonolysis experiments. Thus, we only focused on HOMCHO compounds in the experiments without NOx addition, and the HOMON species measured in the NOx experiments were mainly formed through NO/NO3 reactions instead of nitrate-dimer-charged HOMCHO compounds. In addition, HOM products were grouped according to different carbon numbers to investigate their distribution. C8C10 and C16C20 compounds were regarded as HOM monomers and dimers, respectively, to be consistent with previous research works (Y. Zhao et al., 2018; Molteni et al., 2019). Thus, HOM species discussed in this study are limited to molecules with a formula as Cx>7Hy>7N02Oz>5 (excluding the NO3- reagent ions), which contributed 83 %–91 % of the total measured signals (shaded areas in Fig. 3).

Figure 3(a–c) Mass defect plot of particle-phase signals (60 min average, 230 C) measured in experiment no. 3 (input flow concentration as 120 ppb α-pinene and 33 ppb O3). The data points are identical in panels (a)(c), but colored by the (a) carbon number, (b) hydrogen number, and (c) oxygen number. The area of the markers is proportional to the logarithm of measured raw signals. The grey markers are either unknown peaks (unidentified) or not HOM compounds according to the nomenclature of “HOM” (Bianchi et al., 2019). (d–f) Distribution of signals (normalized to the largest peak) grouped by (d) carbon number, (e) hydrogen number, and (f) oxygen number. The particle-phase measurements are shown as colored bars, while the gas-phase measurements are shown in grey. The shaded areas in panels (d)(f) are the focus of this study.


Finally, elemental ratios were calculated in order to compare the bulk chemical composition of SOA measured by the AMS and the VIA–NO3-CIMS system. Molar O/C, H/C, and N/C ratios of AMS were calculated using the improved Aiken method (IA), with uncertainties of 28 %, 13 %, and 22 %, respectively (Aiken et al., 2008; Canagaratna et al., 2015). Nitrate signals measured by the AMS are almost all from organic nitrates, which is consistent with the estimation of NOx+ ratio method (Farmer et al., 2010; Day et al., 2022). Molar O/C, H/C, and N/C ratios of the NO3-CIMS measurements (signal weighted) were calculated based on the fitted chemical formulas. The uncertainty mainly comes from the accuracy of high-resolution fitting results, relative calibration factors among different HOM compounds (instead of the absolute calibration factors), and the signal-to-noise ratios of each compound.

2.4 Kinetic model and RO2 chemistry

A simple 0-D kinetic box model was used to model α-pinene concentrations and support the interpretation of the experimental results. The chemical reactions and physical parameters are described in Sect. S2. As shown in Fig. 2b, the modeled α-pinene is consistent with the PTR-ToF measurements. Based on the only two α-pinene measurements during the first experiment, modeled α-pinene concentrations were estimated with an accuracy of 10 %, though this will probably be less accurate for the NOx experiments because more reactions need to be considered in the model. The main reactions that will be discussed in the following sections are listed below.

RO2RO4RO6 … (R1a,
RO2(H-shift)R(=O)+OH (R1b,
RO2+RO2R-OH+R(=O)+O2 (R2a,
carbonyl and
RO2+RO2RO+RO+O2 (R2b, alkoxy
RO2+RO2ROOR+O2 (R2c, dimer)
RO2+HO2ROOH+O2 (R3a,
RO2+HO2RO+OH+O2 (R3b, alkoxy
radical and
RO2+NORONO2 (R4a, organic
RO2+NORO+NO2 (R4b, alkoxy
radical and

Peroxy radicals are the key intermediate in α-pinene ozonolysis leading to HOM formation (Ehn et al., 2017; Iyer et al., 2018; Berndt et al., 2018). They can undergo unimolecular autoxidation, forming more oxidized RO2 (Reaction R1a), or termination, forming monomer products (Reaction R1b). They can also undergo bimolecular reactions (Reactions R2–R4) with RO2, HO2, or NO to form closed-shell monomer or dimer products or alkoxy radicals (RO), which may or may not form another RO2 to restart this cycle (Mentel et al., 2015; Berndt et al., 2018; Bianchi et al., 2019). The branching ratios depend on the concentration of reaction partners.

In α-pinene ozonolysis, the fate of RO2 is mainly through unimolecular (Reaction R1a and b) and bimolecular (Reaction R2a–c) reactions. Different α-pinene concentrations will change the relative importance of these two kinds of pathways. Thus, the concentration-dependent distribution of HOM products in both phases was investigated in experiment nos. 1–3 (α-pinene, 53–120 ppb). In experiment no. 4 with CO as an OH scavenger, ozonolysis was largely isolated so that we could focus on O3-derived RO2 and corresponding HOM products. Note that added CO will turn OH to HO2, thus making HO2 a competitive partner to react with RO2 (Reaction R3a and b). In experiment no. 5, NO2 was added under dark conditions to introduce NO3-initiated (formed from the reaction of NO2 and O3) oxidation, forming nitrooxy peroxy radicals (nRO2), which have been proposed not to undergo autoxidation very efficiently (Kurtén et al., 2017). Nevertheless, the fate of nRO2 through bimolecular (Reaction R2a–c) reactions with another RO2/nRO2 would still be expected. Finally, NO was formed after turning on the UV lights (experiment nos. 6–9, inflow VOC/NOx=15.6–1.1), which partly converted RO2 to organic nitrates as N-containing HOM monomers (Reaction R4a) instead of through bimolecular (Reaction R2a–c) reactions with another RO2. O3 to α-pinene ratios (0.28–0.62) that are relatively lower than their distribution in the real atmosphere were used in this work to reduce reactions between NO and O3, which maximizes bimolecular reactions between NO and RO2. Note that the gas-phase HOMs were measured in experiment nos. 6–9 with lights both off and on, whereas the particle-phase measurements were only obtained with the lights on. Experiment no. 5 was conducted with lights off during the entire experiment, which is the only one containing information about particle-phase HOM products from NO3 and α-pinene reactions without NO chemistry. In the following sections, both the identification of gas- and particle-phase HOM products and their relationship will be investigated in detail for each reaction system.

3 Results

3.1 HOM distribution under different conditions

3.1.1α-pinene and O3 dark reactions

Mass defect plots of particle-phase signals measured by the VIA–NO3-CIMS system from α-pinene ozonolysis are given in Fig. 3a–c, which show large differences compared to gas-phase measurements (Fig. S2). In the gas phase, C10H14,16Oz dominates HOM monomers followed by C8H12Oz, while the dimers (much lower than monomers) were almost evenly spread among C17C20 compounds (Fig. 3d). However, in the particle phase, dimers (dominated by C17H26Oz followed by C18,19H26,28Oz) showed comparable or even higher contributions to total HOM signals than monomers (mainly C10 compounds). Similarly, higher dimer than monomer signals of α-pinene SOA were measured in sodiated ion-adducted ([M+Na]+, electrospray ionization) mass spectra (Zhang et al., 2017). In addition, C16H24,26Oz was almost exclusively observed in the particle phase, indicating particle-phase-related sources of these compounds. Oxygen numbers also changed, peaking around O6O7 in the gas phase, but shifted to O7O10 in the particle phase (Fig. 3f). Nevertheless, the signal-weighted O/C of the particle-phase HOMs is lower than that of the gas phase (details in Sect. 3.2), owing to a large shift of C numbers in the particle phase. Last, H numbers (Fig. 3d) are highly correlated with C numbers for HOM products in both the gas and particle phases, as expected. And a small amount of C10H15Oz and C9H13Oz peroxy radical was measured in the gas phase but negligible in the particle phase.

Many elemental compositions identical to the monomers and dimers identified in this work were also reported by other mass spectrometry techniques (summarized in Table S2), though in general, species reported in this work contained more oxygen than in previous publications (Müller et al., 2009; Zhang et al., 2015; Mutzel et al., 2015; Kristensen et al., 2020; Pospisilova et al., 2020). For example, ester dimers with molecular formulas as C17H26O7 and C17H26O8 were identified by an ultrahigh-performance liquid chromatography/electrospray ionization quadrupole time-of-flight mass spectrometer (UHPLC/ESI-qToF-MS) (Kristensen et al., 2020; Kahnt et al., 2018). However, the structure of many ester dimers with five to seven oxygen atoms was proposed to contain carboxylic functional groups at both ends (Kristensen et al., 2016; Zhang et al., 2015), which would possibly be “invisible” to an NO3-CIMS owing to large difficulties forming two hydrogen bonds with the reagent ions (Hyttinen et al., 2015). It remains unclear to what extent the identical elemental compositions reflect identical isomeric structures, given the differences between the methods. Nevertheless, the similarities in detected compositions are encouraging, even though one needs to be careful not to draw direct links to previous observations using different methods.

Figure 4(a–c) Mass spectra of (a) gas-phase (without seed particles), (b) condensed-gas-phase (from the difference between gas-phase mass spectra without and with seed particles, see Sect. 2.2), and (c) particle-phase (at 230 C) measurements from experiment no. 3 (input flow concentration as 120 ppb α-pinene and 33 ppb O3). Gas-phase and condensed-gas-phase mass spectra (30 min average) are normalized to (C10H14O7)NO3 at m/z 308 with m/z 224 and m/z 240 off the scale. Particle-phase mass spectra (60 min average) are normalized to (C17H26O8)NO3 at m/z 420. (d–f) The distribution of HOM products for experiment nos. 1–4, grouped by C numbers, is summarized in (d) for the gas phase, (e) for the condensed gas phase, and (f) for the particle phase. Signals are normalized to the C10 family.


Different initial concentrations of α-pinene were used to investigate the concentration-dependent distribution of HOM products, summarized in Fig. 4d–f. In the gas phase, as more α-pinene reacted, more RO2 was formed in the system, thus making self- and cross-reactions between two RO2 more important, while decreasing the autoxidation (Reaction R1a) and unimolecular termination (Reaction R1b). We indeed see a lower fraction of compounds with large O numbers in the gas phase when increasing the α-pinene concentrations (Fig. S3), while C8 monomers (likely from Reaction R2b followed by fragmentation) and all dimers (from Reaction R2c) increased (Fig. 4d). The concentration-dependent trend of HOM distributions in the gas phase is consistent with that observed at relatively low α-pinene conditions (17–1692 ppt) with ∼30 ppb O3 (Molteni et al., 2019), despite clearly higher α-pinene (53–120 ppb) and O3 (∼33 ppb) concentrations used in this work.

When adding NaCl seed particles to convert more HOM vapors into SOA, mass spectra of the condensable gas phase could be obtained (i.e., the difference of gas-phase measurements between without and with seed particles, Fig. 4b). Low-volatility monomers and almost all dimers (with roughly m/z >350 Th including the reagent ion NO3-) showed comparable, largely kinetically limited, and irreversible condensation loss on the seed particles, similar to results from an earlier study (Peräkylä et al., 2020). The mass spectra of condensed-gas-phase HOMs were in general comparable to those of the gas phase (Fig. 4b vs. Fig. 4a and Fig. 4e vs. Fig. 4d), though with a slightly higher dimer contribution. However, the particle-phase HOM distribution was dramatically different from the (condensed-)gas-phase measurements, and measured dimer concentrations were even higher than monomers (Fig. 4f). With more α-pinene reacted, the enhancement of C16C19 dimers in the particle phase was much larger than that observed in the gas phase, while the particle-phase O-number distribution did not show obvious concentration-dependent changes among different experiments (Fig. S3). In addition, C17H26O9 was identified in both gas and particle phases, whereas C17H26O7,8 was only detected in the particle phase. These compounds have also often been identified from filter measurements (Müller et al., 2009; Zhang et al., 2015; Mutzel et al., 2015; Kristensen et al., 2020). All these particle- and gas-phase comparisons raise an interesting question – what is the source of those C16C19 dimers?

Figure 5Mass spectra of (a) gas-phase (30 min average) measurements before (green) and after (pink) adding 100 ppm CO in experiment no. 4 (input flow concentration as 120 ppb α-pinene and 33 ppb O3), normalized to (C10H14O7)NO3 at m/z 308 with m/z 224 and m/z 240 off the scale, and (b) particle-phase (60 min average) measurements with (pink) and without (green) CO, normalized to (C10H16O9)NO3 at m/z 342 and (C17H26O8)NO3 at m/z 420, respectively. Note that the oxidation rate of α-pinene decreased to about half due to the decreased OH oxidation after adding CO (assuming the OH yield to be ∼0.8 from ozonolysis of α-pinene). Therefore, experiment no. 2 (80 ppb α-pinene) was chosen for the particle-phase comparison because of comparable SOA concentrations.


The evenly distributed C17C20 HOM dimers in the gas phase and their extremely low volatilities (Peräkylä et al., 2020; Hyttinen et al., 2021) would have us expecting a similar distribution in the particle phase. However, the very different HOM distribution measured in the two phases implies that particle-phase reactions are taking place. We cannot rule out the possibility that our VIA sampling setup is perturbing the true distribution, and these limitations are discussed in more detail in Sect. 3.4. Earlier studies have speculated on different processes forming dimers in the particle phase. For example, C17H26O8 (nominal mass at 358 amu, m/z 420 in Fig. 4), which showed the highest signal in the dimer range (negligible in the gas phase), was also reported as the most abundant oligomer in α-pinene SOA measured by high-performance liquid chromatography and Fourier transform ion cyclotron resonance–mass spectrometry (HPLC/FTICR-MS) (Müller et al., 2009). In that study, liquid chromatography followed by mass spectrometry showed that C8H12O4 and C9H14O4 (cis-pinic acid and isobaric compounds detected at m/z 185) are monomeric units that make up this C17 dimer. It was later proposed that C8H12O4 could be terpenylic acid (and isobaric compounds detected at m/z 171) (Yasmeen et al., 2010; Beck and Hoffmann, 2016). However, the proposed esterification process needs aqueous and acid conditions to turn the lactone group of terpenylic acid into two alcohol moieties (Beck and Hoffmann, 2016), which is not available in this study (dry NaCl seed particles). In addition, terpenylic acid was proposed to be formed either through OH-initiated oxidation of α-pinene or an O3-initiated pathway of α-pinene oxide (yield ∼2 %) (Claeys et al., 2009). However, in the CO (used as an OH scavenger) experiment (no. 4, discussed in the next section), when both these pathways were very limited, C17H26O8 was still observed as the highest dimer peak in Fig. 5b. In addition, it has been shown in other studies that a dominate role of dimers (including C17H26O8) in the particle phase was primarily determined from ozonolysis of α-pinene (Kristensen et al., 2014; Zhang et al., 2017).

Recently, Claflin et al. (2018) used derivatization–spectrophotometric methods to quantify the distribution of different functional groups in very-high-concentration α-pinene SOA (∼3 mg m−3). They compared the measurements to the modeled results of the Master Chemical Mechanism and proposed that hydroperoxides and peroxycarboxylic acids along with aldehydes and ketones could be converted to carboxyl monomers and ester dimers through the Baeyer–Villiger reaction in SOA. This would be an explanation of those “newly formed” dimers measured in the particle phase, which may also be important under atmospheric conditions (i.e., low SOA concentrations). Furthermore, particle-phase decomposition of more carbon-containing HOM compounds (e.g., C10 in the monomer range and C20 in the dimer range) was proposed as an important decay pathway of α-pinene SOA (Pospisilova et al., 2020), which could largely explain the relative enhancement of C16C19 compared to C20 compounds. However, the lifetime of SOA particles is different between the two studies. For example, C16C17 signals peak after ∼2 h of the α-pinene ozonolysis in their batch-mode experiments, whereas the residence time is ∼1 h for the continuous-mode experiments conducted in this work. Nevertheless, about half of the compounds were proposed to have half-lives of less than 1 h (Pospisilova et al., 2020). If the thermal energy supplied during the evaporation of SOA within the VIA can promote this decay process, then the observed particle-phase HOM distribution would be expected to shift to lower C numbers.

Although the above discussion mainly focused on C17 compounds, C18C20 HOM dimers observed in the gas phase were still identified in the particle phase. Thus, the particle-phase dimers measured in this work may be partly intact HOM dimers formed and condensed from the gas phase (Berndt et al., 2018; Jokinen et al., 2014) and partly particle-phase-formed dimers, which are multifunctional organic compounds being detected by an NO3-CIMS (and thus were regarded as HOMs). However, as discussed in Sect. 2.2, some of the enhancement of C16C19 compounds observed in the particle phase is likely due to a higher detection efficiency for HOM dimers than monomers with the VIA setup at 230 C. In order to understand this “dimer enhancement” better and to extend the results from the α-pinene ozonolysis system (Pospisilova et al., 2020) to various conditions, we conducted experiments wherein we modified the dimer to monomer (D/M) ratios of HOMs in the gas phase by adding CO or NO to the system (as discussed in the following sections) to investigate the effects of the corresponding D/M ratios in the particles.

3.1.2α-pinene and O3 dark reactions with CO

In experiment no. 4, CO was used as an OH scavenger (i.e., to isolate O3 initiated reactions) to test the hypothesis that O3-derived RO2 and corresponding monomers are important for dimer formation in the particle phase (Kristensen et al., 2014; Zhang et al., 2017) and to change the gas-phase HOM distribution. α-Pinene and O3 were first added into the chamber, similar to experiment no. 3, whereafter CO was added to largely shut down OH-initiated formation of HOMs. The added CO increases HO2/RO2 ratios compared to the pure α-pinene ozonolysis systems (roughly by a factor of 104 estimated by the kinetic model), making HO2 a competitive partner to react with RO2 (Reaction R3a and b). Thus, lower relative concentrations of dimers were observed (Fig. 5a). Total HOM concentrations also decreased after adding CO, likely due to the decreased oxidation rate of α-pinene (Fig. S4a). However, enhancement of C16C19 dimers compared to monomers was still observed in the particle phase (Figs. 5b and 4f). Furthermore, the peaks identified in the particle phase were almost the same as the ones without CO, strongly suggesting that ozonolysis products of α-pinene are important and perhaps necessary for the formation of these dimers (Kristensen et al., 2014; Zhang et al., 2017). In fact, the mass spectra of the CO experiment (no. 4) correlated well with the ones of experiment no. 2 without CO as well as with r2=0.82, 0.75, and 0.80 for gas-phase, condensed-gas-phase, and particle-phase measurements, respectively.

In addition, although the majority of HOM products decreased largely in the gas phase after adding CO, C10H16O8,10 increased significantly (Fig. S4a), which was also obvious from the time series (Fig. S5). This rapid increase with CO suggested that C10H15O8,10 existed as dominant RO2 in the gas phase and was terminated rapidly by HO2 forming hydroperoxides (Reaction R3a). On the other hand, C10H18Oz and C20H34Oz compounds were only formed through reactions of OH-derived RO2 and therefore decreased after adding CO. Although C10H14Oz and C20H30Oz compounds were formed only through ozonolysis of α-pinene (Molteni et al., 2019), a general decrease was also observed, likely owing to the shift from RO2 regime (i.e., RO2 autoxidation and RO2 cross- or self-reaction) to HO2 regime (i.e., RO2 and HO2 termination reaction). The decreased RO2 autoxidation is supported by the results in Fig. S5, showing that C10H14O>7 compounds are in general less oxidized with CO addition. The decreased RO2 cross- or self-reaction is supported by the results in Figs. S5 and 5, showing that the gas-phase dimers largely decreased with CO addition.

Figure 6(a–c) Mass spectra of (a) gas-phase (without seed), (b) condensed-gas-phase (from the difference between spectra without and with seed particles), and (c) particle-phase (at 230 C) measurements from experiment no. 7 (input flow condition of 120 ppb α-pinene, 33 ppb O3, and 17.3 ppb NO2 with UV lights on). Gas-phase and condensed-gas-phase mass spectra (30 min average) are normalized to (C10H14O7)NO3 at m/z 308 with m/z 240, and/or m/z 208 and m/z 224, off the scale, with peaks larger than 420 Th being multiplied by a factor of 5. Particle-phase mass spectra (60 min average) are normalized to (C10H16O7)NO3 at m/z 310 with m/z 339 off the scale. Nitrogen-containing ions (CxHyNOz, i.e., HOMON) are plotted downward, while the other ions are plotted upwards. (d–f) The distribution of HOM products (varying initial α-pinene to NOx ratios from 15.6 to 1.1), grouped by carbon numbers, in the (d) gas phase, (e) condensed gas phase, and (f) particle phase. Signals are normalized in each experiment to the C10 family of HOMCHO compounds (green bars), and the blue bars (HOMON) are stacked on the top of the HOMCHO.


3.1.3α-pinene and O3 reactions with NO (UV lights on)

NO (generated from the photolysis of NO2) was introduced into the α-pinene ozonolysis system in experiment nos. 6–9, and it acted similarly to HO2 in the CO experiment to partly terminate RO2 into monomers instead of forming dimers in the gas phase. Although a relatively smaller branching ratio towards the formation of HOMON monomers (Reaction R4a) than RO (Reaction R4b) would be expected, one more N atom makes the HOMON monomers (dominated by C10H15,17NOz and C9H13,15NOz compounds, Fig. 6) easier to track compared to the enhanced hydroperoxides in the CO experiment. As shown in Fig. 6d, with lower initial AP/NOx ratios, the contribution of HOMON monomers increased and HOMCHO dimers decreased in the gas phase. Similar effects of NO – terminating RO2 and forming organic nitrates instead of dimers, thus suppressing SOA formation – were reported from previous studies (Ehn et al., 2014; D. Zhao et al., 2018; Pullinen et al., 2020). The condensed gas phase followed the patterns of the gas-phase measurements.

Particle-phase HOMs again showed relatively higher contributions of dimers (C16C20 compounds) compared to the gas phase (Fig. 6f vs. Fig. 6d). However, different from experiment nos. 1–4, NO was used in experiment nos. 6–9 to terminate RO2 to RONO2, which is not as effective as a particle-phase precursor as HOMCHO monomers to form dimers through the Baeyer–Villiger reaction in SOA (Claflin et al., 2018). Consequently, less “enhancement” of C16C19 HOMCHO compounds in the particle phase was observed compared to experiments without NOx (Fig. 6f vs. Fig. 4f). In addition, highly functionalized organic nitrates observed in the particle phase have been found to decompose within 2–4 h based on ambient measurements (Lee et al., 2016), suggesting that the formation of HOMON might be larger than we detected.

3.1.4α-pinene and NO3 dark reactions (UV lights off)

Particle-phase HOMs from NO3-initiated oxidation were investigated by adding NO2 into the α-pinene ozonolysis system under dark conditions (i.e., UV lights off) in experiment no. 5. NO3 oxidation of alkenes almost exclusively undergoes electrophilic addition to the double bond instead of H abstraction (Kerdouci et al., 2010), and thus multigeneration oxidation by NO3/O3 should be negligible. In experiment nos. 6–9, α-pinene, O3, and NO2 (7.6–46.6 ppb) were added into the chamber until a steady state was reached, whereafter the UV lights were turned on to photolyze NO2 and NO3 to NO (results discussed in Sect. 3.1.3). Thus, only gas-phase measurements from NO3-initiated oxidation were obtained from those experiments (Fig. 7d), whereas experiment no. 5 was conducted with UV lights off during the entire period, making it the only one with particle-phase HOM measurements of the α-pinene and NO3 reactions (Fig. 7f).

Figure 7(a–c) Mass spectra of (a) gas-phase (without seed), (b) condensed-gas-phase (from the difference between spectra without and with seed particles), and (c) particle-phase (at 230 C) measurements from experiment no. 5 (input flow condition of 120 ppb α-pinene, 33 ppb O3, and 7.6 ppb NO2 with UV lights off). Note that the y axes of HOMCHO (green spectrum, upward) and HOMON (brown spectrum, downward) are on different scales. Gas-phase and condensed-gas-phase mass spectra (30 min average) are normalized to (C10H14O7)NO3 at m/z 308, with peaks larger than 420 Th being multiplied by a factor of 3. Particle-phase mass spectra (60 min average) are normalized to (C10H16O9)NO3 at m/z 342. (d–f) The distribution of HOM products (varying initial α-pinene to NOx ratios from 15.8 to 1.1), grouped by carbon numbers, in the (d) gas phase, (e) condensed gas phase, and (f) particle phase. Signals are normalized to the HOMCHO C10 family. The UV lights were off during the entire experiment, making experiment no. 5 (HOMON as brown bars) the only one with particle-phase HOM measurements from α-pinene and NO3 reactions.


For both NO and NO3 experiments, HOMON compounds were dominated by compounds with only one nitrogen atom (94.5 % ± 0.9 %) in both gas and particle phases. This result indicates that NO termination of NO3-derived nitrooxy-RO2 was negligible in both systems and likewise that HOM dimer formation through cross-reactions of two nRO2 compounds was unlikely. Note that many previous studies used N2O5 as the NO3 source (and often with concentrations higher than VOCs) to avoid O3-initiated oxidation, and thus CxHyN2Oz compounds (e.g., C20H32N2O9,10) were the largest signals in the dimer range, formed by self- and/or cross-reactions of two nRO2 compounds (Claflin and Ziemann, 2018; Takeuchi and Ng, 2019; Bell et al., 2022). O3-derived RO2 still contributed largely to HOMs in this work, and thus cross-reaction of nRO2 with RO2 was the main process forming dimers (with only one N atom, e.g., C19H31NOz and C20H31NOz). In addition, since HOMON signals generally increased after turning on the UV lights (Fig. S6), peroxy acyl nitrates (PANs) formed through NO2 termination of RO2 (Rissanen, 2018) were likely less important than NO termination due to lower reaction rates and lower thermal stability of the products (Atkinson, 2000; Orlando and Tyndall, 2012; Berndt et al., 2015).

In the NO3 experiment (experiment no. 5, Fig. 7), C10 compounds dominated HOMCHO in the monomer range in both gas and particle phases, while C9 and C10 compounds were the largest HOMON monomers. Similarly, C10H15,17NOz and C9H13,15NOz were identified as the main HOMON products during NO3-initiated α- and β-pinene oxidation using a FIGAERO–iodide-CIMS for gas- and particle-phase measurements (Boyd et al., 2015; Nah et al., 2016; Takeuchi and Ng, 2019) and when using an EESI-ToF for SOA measurements at the Hyytiälä boreal forest site (Pospisilova et al., 2020). A detailed comparison of HOMON peaks identified in the particle phase from this work with other techniques is summarized in Table S3. Again, C16C18 compounds were nearly exclusively measured in the particle phase along with a relative enhancement of C19 compounds compared to the gas phase, indicating potential particle-phase-related processes.

Figure 8Summary of (a) total HOM concentrations estimated in the gas phase, condensed gas phase, and particle phase (different scales were used for different phases); (b) dimer to monomer (D/M, i.e., C16-C20/C8-C10) ratios; (c) particle-phase HOM and SOA measurements. The evaporated SOA mass was calculated from AMS measurements (i.e., the mass difference between VIA and bypass modes). Experiment numbers are given in panels (a) and (b). Shaded areas in panel (a) represent experiments with initial α-pinene concentrations of 120 ppb. The HOM concentrations are given in absolute values here to be able to compare the different experiments more quantitatively, but the large uncertainties (at least a factor of 3) need to be kept in mind. The gas-phase HOM concentration is used as the x axis in (b) as a surrogate for the overall α-pinene reaction rate, which could not be plotted directly due to the lack of VOC measurement. Grey solid lines in panel (b) only serve as guides to connect experiments with similar conditions.


3.1.5 Summary of dimer/monomer distributions

In this section, the dimer to monomer (D/M) ratio was calculated for each experiment to relate the distribution of HOM products in both phases. Overall, D/M ratios observed in the particle phase followed the trend of the gas phase for all experimental conditions. As dimers condensed more readily than monomers, the gas-phase D/M ratios decreased after adding seed particles (Fig. S7d), and the condensed-gas-phase D/M ratios (grey markers in Fig. 8b) were roughly 1.5-fold compared to the gas phase. However, the D/M ratios measured in the particle phase were 2–9 times as high as those observed in the (condensed) gas phase (Fig. S8). Interestingly, the experiments wherein we observed the lowest gas-phase D/M ratios (experiment nos. 4, 8, 9) were the ones wherein the particle-phase D/M enhancement was the largest. In the case that there was dimerization taking place in the particles, this process should indeed be seen most clearly when the quantity of condensing dimers was the lowest. Overall, these highest discrepancies between different phases are larger than the expected underestimation of monomer signals (by a factor of ∼2 estimated by comparing the measurements between 230 and 170 C, as shown in Fig. 2c for C10 compounds). Nevertheless, further investigations will be needed to study to what extent this enhancement could be attributed to particle-phase chemistry.

One striking feature of Fig. 8b is that despite the D/M ratio of gas-phase HOMs varying by a factor of 3 between different experiments (i.e., range of y values for red markers in Fig. 8b), the relative changes in D/M ratios between different experiments (for the same phase) were clearly lower. For example, between experiment no. 1 and no. 3, the gas-phase D/M ratio increased by ∼50 % (from 0.2 to 0.3) and the particle-phase D/M ratio increased by a very similar amount of ∼54 % (from 1.1 to 1.7). We can only speculate about the underlying reasons behind this behavior. One possibility is that there is dimer formation in the particles that scales suitably to produce the observed results. Another possibility is that our sensitivity to HOM monomers in the particle phase is lower than for HOM monomers in the gas phase. As indicated earlier, the average C-atom content in the HOM dimers was lower in the particles than in the gas phase under all conditions. The loss of C atoms is unlikely to be limited to the dimers, and similar changes in the monomers can be expected (whether through particle-phase chemistry or thermal decomposition). The loss of a few functional groups from a HOM monomer can potentially make it undetectable by the NO3-CIMS, which in turn would cause an increase in the observed D/M ratio. Future studies will hopefully be able to shed more light on this matter. The potential role of thermal decomposition upon heating cannot be ruled out and will be discussed further in Sect. 3.4.

In the NO experiments (nos. 6–9 with UV lights on), D/M ratios of the condensed-gas-phase HOMs changed the most by nearly a factor of 4 (Fig. 8b). However, the concurrent decrease in particle-phase D/M ratios was smaller, closer to a factor of 2. This change is also clear from Fig. S8. If there was particle-phase dimer formation taking place, the effect should be most visible when the gas-phase dimer contributions are the lowest, as in these experiments. While the very high NOx/VOC ratios in these experiments make the direct comparison to other experiments hard, this can be seen as an indication that particle-phase dimer formation is indeed taking place, as has been suggested earlier (Kalberer et al., 2004; Claflin et al., 2018). It should also be noted that in these experiments, the gas- and particle-phase absolute concentrations clearly changed from other experiments (Fig. 8a). HOM concentrations (HOMCHO+HOMON) increased 13 %–81 % in the gas phase, whereas particle-phase HOMs decreased 33 %–40 % (and SOA decreased 11 %–50 %, Fig. S7) compared to the reference α-pinene and O3 experiments (nos. 1 and 3). This indicates a higher average volatility of the observed gas-phase HOMs, largely explainable by suppressed formation of low-volatility HOMCHO dimers and increased formation of more volatile HOMON monomers. Exactly how this may impact the D/M ratios in gas- and particle-phase HOMs remains an open question.

As there are still uncertainties relating to the VIA response, e.g., in correctly accounting for wall losses of vapors in the current experimental setup (especially within the VIA), only a qualitative comparison was given here. As shown in Fig. 8c, ∼80 % of SOA evaporated within the VIA system based on AMS measurements, which is consistent with the integrated mass based on SMPS datasets (Fig. S7b). However, particle-phase HOM concentrations measured by the VIA–NO3-CIMS were much lower (by a factor of ∼5–6, accounting for the dilution and assuming an average molecular mass of HOM compounds of 300 g mol−1) compared to the AMS measurements. This difference is large enough that even after accounting for our large uncertainties in quantification, we expect that a noticeable fraction of the particle-phase products is not detected using this system. Vapor losses to the walls after evaporation and the selectivity of our ionization are expected to be the two main reasons for this. More detailed characterization of this inlet system will be investigated in future studies in order to evaluate if the wall losses can either be avoided or accounted for. Nevertheless, the trend of particle-phase HOMs is comparable to the SOA measurements (Fig. 8c), with the largest discrepancies observed under high SOA loadings with NOx added.

3.2 Elemental composition of HOMs

In this section, van Krevelen diagrams are used to investigate the bulk chemical properties of HOMs measured in both gas and particle phases and are compared to the more routine elemental analysis from the AMS (DeCarlo et al., 2006; Aiken et al., 2007, 2008; Canagaratna et al., 2015).

As shown in Fig. 9a, gas-phase HOM monomers formed rapidly after the injection of α-pinene and O3, with bulk chemical composition stabilizing at elemental ratios resembling C10H15O8–9. Dimers followed the H/C of monomers but showed lower O/C ratios, as has also been observed in earlier studies (Jokinen et al., 2014; Berndt et al., 2018). In the particle phase, the chemical compositions of HOMs measured at different temperatures were quite comparable, and thus the datasets obtained at 230 C were used to represent the particle-phase HOM measurements. Since the elemental ratios of HOM measurements are relatively stable 1.5 h after injection of gas precursors, signal-weighted means were calculated for each phase after reaching a steady state for each experiment separately (Fig. 9b and c). In general, it is interesting that all datasets showed comparable H/C ratios (1.5±0.1) but a relatively large range of O/C ratios. In particular, O/C ratios of HOMs measured in the particle phase (purple markers in Fig. 9b) are lower compared to the gas-phase (red markers) and condensed-gas-phase (grey markers) measurements (0.63–0.80 vs. 0.76–1.02). The AMS-measured SOA showed the lowest O/C ratios (0.34–0.48), which are comparable with previous studies (Alfarra et al., 2006; Chhabra et al., 2010), as summarized in Table S4 and Fig. S10. One possible explanation for the inconsistence of O/C ratios between AMS and CIMS measurements is that the VIA–NO3-CIMS measured only the most oxidized part of the SOA (as discussed in Sect. 3.1.5).

Figure 9The van Krevelen diagrams of the VIA–NO3-CIMS and AMS data. (a) Gas-phase HOMs (10 s averaged data points) and SOA measured by AMS (20 s averaged data points) from experiment no. 1. The SOA and the gas-phase HOM data are colored by the time after α-pinene and O3 injection, while the particle-phase HOMs are colored by the temperature of the VIA. (b) Average “bulk” HOM and SOA elemental ratios for all experiments. (c) Average gas-phase (red, 30 min), condensed-gas-phase (grey, 30 min), and particle-phase (purple, 60 min) HOM elemental ratio separated into monomers (C8C10) and dimers (C16C20).


HOM measurements were also separated into monomers and dimers for more detailed comparisons (Fig. 9c). In α-pinene ozonolysis experiments, the chemical compositions of gas-phase HOMs are comparable under different initial α-pinene concentrations (red circles in Fig. 9c). The condensed-gas-phase monomers showed slightly higher O/C ratios, while dimers showed comparable O/C ratios compared to the gas phase (red vs. grey circles), which is consistent with the volatility distribution of HOM products (Peräkylä et al., 2020). However, a small O/C gap was observed between the particle phase and the (condensed) gas phase for dimers (0.50–0.51 vs. 0.58–0.59). In experiment no. 4, adding CO largely shut down OH-derived RO2, which led to lower H/C ratios of gas-phase dimers compared to that before CO addition (Fig. S8a). On average, the H/C ratios of dimers decreased from 1.52 to 1.48 in the gas phase and decreased from 1.55 to 1.51 in the particle phase. The AMS measurements did not show detectable effects after adding CO. Again, the gas and particle phases showed a small gap in the dimer range (red vs. purple square in Fig. 9c) as in experiment nos. 1–3.

In NOx experiments, H/C ratios of both gas-phase HOM monomers and dimers decreased after turning on the UV lights (Fig. S8b) owing to the interruption of NO3-initiated oxidation (i.e., NO3-formed nRO2 radicals have one more H atom than O3-derived RO2). However, all particle-phase measurements (purple diamonds and triangles in Fig. 9c) were relatively comparable with other experiments (especially for dimers), indicating similar particle-phase transformations after the condensation of HOMs from the gas phase. On the other hand, in both NO3 (lights off) and NO (lights on) experiments, higher O/C ratios were observed in the monomer range compared to experiments without NOx because of three more O atoms from the nitrate functional group. In addition, higher N/C ratios were observed in both the gas (0.037–0.07 vs. 0.018–0.02) and particle phase (0.01–0.04 vs. 0.01) with UV lights on compared to those without UV lights, confirming that more HOMON was formed through NO and RO2 reactions than NO3 oxidation. Correspondingly, higher O/C ratios of SOA were observed with UV lights on compared to the dark NO3 experiment (0.40–0.48 vs. 0.34–0.41).

Figure 10Scatter plots of organic nitrate observations with the VIA–NO3-CIMS and AMS. (a) AMS-measured nitrate mass vs. organic mass during NOx experiments (nos. 5–9) with UV lights off. (b) Same as (a), but with UV lights on. (c) NO+ vs. NO2+ ions measured by the AMS, including experiments with UV lights both off and on. (d) Molar fraction of organic nitrate (HOMON) to total organic signals (HOM=HOMCHO+HOMON) measured by the VIA–NO3-CIMS system vs. the ratio of nitrate to organics measured by the AMS ((nitrate/62)/(SOA/300)).


3.3 Organic nitrate (ON) measurements

Finally, organic nitrates measured by the AMS and the VIA–NO3-CIMS system were compared to evaluate the performance of this novel system. Based on AMS measurements, nitrate mass tracked well with organics (Fig. 10a and b) for each experiment separately, indicating that nitrate signals were from organic nitrates. The nitrate / organic ratio in the AMS also increased very clearly as the NOx/VOC ratio in the chamber increased. The nitrate / organic mass ratios increased from 0.012–0.061 to 0.018–0.075 after turning on the UV lights, in agreement with the earlier discussion that more intensive HOMON formation took place in NO experiments than in NO3 experiments. The NO+/NO2+ ratios, a marker for the contribution of organic nitrates to the measured nitrate signal, observed in experiment nos. 6–9 did not show discrepancies between UV lights on and off (Fig. 10c) and were well separated from the dataset of ammonium nitrate calibration (5.2–5.6 vs. 1.6).

Assuming an average molar mass of 300 g mol−1 for organic molecules, the molar fraction of ON to total organic aerosols ((nitrate/62)/(SOA/300)) was estimated to be 5.8 %–30 % for NO3 experiments and 8.7 %–36 % for NO experiments based on AMS measurements. Interestingly, the molar fraction of HOMON to total HOM signals measured in both the gas (circles in Fig. 10d) and particle phase (squares in Fig. 10d) by the VIA–NO3-CIMS correlated well with the above AMS measurements, suggesting that chemical compositions of gas- and particle-phase HOMs (i.e., relative contribution of HOMCHO and HOMON) were quite comparable. Note that the slope of the fitted line is sensitive to several factors, including different calibration factors between HOMCHO and HOMON and the estimated average molar mass of SOA. Thus, the value should be only qualitatively interpreted. We also note that some of the nonzero intercept in Fig. 10d (16 %) is likely contributed by charging in the NO3-CIMS by the nitrate dimer (HNO3NO3-), which is higher than that in α-pinene ozonolysis experiments (estimated to be 4.3 % ± 1.5 %). It is possible that this ratio would increase further in NOx experiments if there was HNO3 formed at some amount in the gas phase. Finally, neither the NO+/NO2+ nor the ON molar fraction analysis showed any clear differences between the NO and NO3 experiments based on AMS and NO3-CIMS datasets. Thus, other parameters (e.g., UV lights on or off in the chamber or hour of the day in the atmosphere) are needed to distinguish HOMON formed by NO3 oxidation from that by NO termination of RO2.

3.4 Discussion on the factors that may affect the HOM detection

Thermal decomposition is a well-known issue with techniques based on the evaporation of molecules from the particle phase to identify the chemical composition of vapors, especially for labile organic mixtures. It remains unclear to what extent the thermal decomposition of SOA happened under different temperatures and/or if the thermal desorption techniques could promote particle-phase reactions. However, if thermal decomposition did play an important role in this VIA–NO3-CIMS system, we would expect more decomposition of dimers (labile ROOR compounds) than monomers, in particular at the highest temperature. Yet, we observed much higher dimer / monomer ratios in the particle phase than the gas phase, suggesting that we might instead “enhance” dimers if the thermal decomposition primarily removed monomers from our sensitivity window.

In Sect. 3.2, lower O/C ratios of the particle-phase HOMs were observed compared to the gas-phase HOMs, which could partly be attributed to the thermal decomposition of organic compounds within the VIA. The carbonyl, peroxide, esters, carboxyl, and hydroxyl groups were ubiquitous functional groups identified in α-pinene SOA under various conditions (Claflin et al., 2018). Decarboxylation of C(= O)O functional groups may play a relatively more important role than the dehydration of hydroxyl (with H2O being the main thermal decomposition product) owing to their expected higher contributions to SOA. Concurrent formation of CO, H2O, and CO2 from decarboxylation would decrease both the O/C and H/C ratios for the particle-phase measurements, which was observed at 200 C on the vaporizer of the AMS (Canagaratna et al., 2015) and in the FIGAERO-CIMS (Stark et al., 2017). With proper combinations of C(= O)OH and C(= O)OR thermal decomposition, it is possible to decrease O/C as well as slightly increase H/C (e.g., on average losing more CO2 or CO than H2O).

In addition, thermal decomposition of peroxide oligomers was observed in the thermogram of acetate–FIGAERO measurements, with an estimated dissociation temperature around 80 C for O–O bonds (Lopez-Hilfiker et al., 2015). However, large quantities of C16C19 dimers measured in this work suggested that these labile peroxides transferred to other more stable functional groups in SOA or that the much shorter residence time at elevated temperature in the VIA (less than 0.2 s), as well as sampling without surface contact, may lead to less thermal decomposition compared to the traditional collection and desorption methods (Häkkinen et al., 2022). Nevertheless, it is clear that we need further investigations to determine if particle-phase processing or thermal decomposition (or other hardware effects) is the larger cause for the changes observed between the particle and (condensed) gas phase in our work. In particular, the temperature-dependent sensitivity (including evaporation and transmission efficiencies) for different types of organic molecules will need to be characterized in future works.

4 Conclusion

Combined gas- and particle-phase HOM measurements were conducted using the novel VIA combined with an NO3-CIMS in this study. α-Pinene ozonolysis was studied under different conditions, including using CO as an OH scavenger and varying NOx concentrations with and without UV lights to perturb the oxidation chemistry and gas-phase dimer formation. Within the 50 min residence time of the chamber, we observed distinct differences between HOMs in particles and the HOMs that were condensing. In particular, we noted clearly enhanced C16C19 HOM dimers in SOA that were not observed in the gas phase. This “enhancement” might be partly attributed to a slightly higher sensitivity to dimers than monomers using the VIA system. However, different chemical composition identified between two phases implies the existence of potential particle-phase chemistry. In addition, gas-phase dimer formation was considerably suppressed in both the CO and NO experiments, and this also led to decreases in particle-phase dimers, yet dimers still made up a considerable fraction of the observed SOA.

In addition to the generally shorter carbon skeletons of the particle-phase dimers (mainly C16C19) compared to the gas phase (mainly C19C20), average O/C ratios of the HOMs (especially in the dimer range) also decreased slightly in the particle phase. Earlier studies have proposed that, e.g., Baeyer–Villiger reactions could convert peroxycarboxylic acids and hydroperoxides to ester dimers in reactions with aldehydes and ketones (Claflin et al., 2018; Bakker-Arkema and Ziemann, 2020), which is not inconsistent with the results observed in this study. Our results indicate that particle-phase reactions are taking place under the timescales probed here, with some of the reactions potentially leading to the formation of new dimers, while some reactions may be causing loss of small fragments (e.g., C20 dimers forming C17 dimers). These predominant C17H26Oz compounds identified in the particle phase, which have often been reported by previous offline measurements, might be related to HOM dimer formation in both the gas and particle phases. However, the new VIA–NO3-CIMS system used in this work will require more detailed characterization in order to better understand how the thermal desorption and wall effects may modify the HOM distributions from those existing in the particles. The NO3-CIMS is known to be selective towards the most oxygenated molecules, which also means that we are likely not detecting all the evaporating compounds. This is also indicated by the measured O/C ratios being clearly higher than those measured by an Aerodyne AMS. However, the measured organic nitrate fraction measured by the VIA–NO3-CIMS was found to track those measured by the AMS. Taken together, we believe that this system is a promising technique for combined online gas- and particle-phase HOM measurements.

Data availability

Data are available upon request from the corresponding authors.


The supplement related to this article is available online at:

Author contributions

ME and JZ designed the study. ME, JK, JEK, MC, and DR supported the experiment setup and analysis methods. JEK built the first version of the VIA. JZ, EH, and FG conducted the experiments. JZ analyzed the data. JZ prepared the paper with contributions from all co-authors.

Competing interests

Jordan Krechmer, Manjula Canagaratna, and Douglas Worsnop work for Aerodyne Research, Inc., which developed and commercialized the VIA used in this study.


Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.


Jian Zhao thanks Lauri Franzon and Otso Peräkylä for helpful discussions about the experiments and results.

Financial support

This work was supported by funding from the Academy of Finland (grant nos. 317380, 320094, 325656, 345982, and 346370) and a University of Helsinki 3-year grant (75284132). Ella Häkkinen thanks the Vilho, Yrjö, and Kalle Väisälä Foundation for financial support. Frans Graeffe acknowledges Svenska Kulturfonden (grant nos. 167344 and 177923) for financial support.

Open-access funding was provided by the Helsinki University Library.

Review statement

This paper was edited by Ivan Kourtchev and reviewed by two anonymous referees.


Aiken, A. C., DeCarlo, P. F., and Jimenez, J. L.: Elemental analysis of organic species with electron ionization high-resolution mass spectrometry, Anal. Chem., 79, 8350–8358,, 2007. 

Aiken, A. C., Decarlo, P. F., Kroll, J. H., Worsnop, D. R., Huffman, J. A., Docherty, K. S., Ulbrich, I. M., Mohr, C., Kimmel, J. R., and Sueper, D.: O/C and OM/OC ratios of primary, secondary, and ambient organic aerosols with high-resolution time-of-flight aerosol mass spectrometry, Environ. Sci. Technol., 42, 4478–4485,, 2008. 

Alfarra, M. R., Paulsen, D., Gysel, M., Garforth, A. A., Dommen, J., Prévôt, A. S. H., Worsnop, D. R., Baltensperger, U., and Coe, H.: A mass spectrometric study of secondary organic aerosols formed from the photooxidation of anthropogenic and biogenic precursors in a reaction chamber, Atmos. Chem. Phys., 6, 5279–5293,, 2006. 

Atkinson, R.: Atmospheric chemistry of VOCs and NOx, Atmos. Environ., 34, 2063–2101,, 2000. 

Bakker-Arkema, J. G. and Ziemann, P. J.: Measurements of Kinetics and Equilibria for the Condensed Phase Reactions of Hydroperoxides with Carbonyls to Form Peroxyhemiacetals, ACS Earth Space Chem., 4, 467–475,, 2020. 

Beck, M. and Hoffmann, T.: A detailed MSn study for the molecular identification of a dimer formed from oxidation of pinene, Atmos. Environ., 130, 120–126,, 2016. 

Bell, D. M., Wu, C., Bertrand, A., Graham, E., Schoonbaert, J., Giannoukos, S., Baltensperger, U., Prevot, A. S. H., Riipinen, I., El Haddad, I., and Mohr, C.: Particle-phase processing of α-pinene NO3 secondary organic aerosol in the dark, Atmos. Chem. Phys., 22, 13167–13182,, 2022. 

Berndt, T., Richters, S., Kaethner, R., Voigtländer, J., Stratmann, F., Sipilä, M., Kulmala, M., and Herrmann, H.: Gas-Phase Ozonolysis of Cycloalkenes: Formation of Highly Oxidized RO2 Radicals and Their Reactions with NO, NO2, O2, and Other RO2 Radicals, J. Phys. Chem. A, 119, 10336–10348,, 2015. 

Berndt, T., Richters, S., Jokinen, T., Hyttinen, N., Kurten, T., Otkjaer, R. V., Kjaergaard, H. G., Stratmann, F., Herrmann, H., Sipila, M., Kulmala, M., and Ehn, M.: Hydroxyl radical-induced formation of highly oxidized organic compounds, Nat. Commun., 7, 13677,, 2016. 

Berndt, T., Mentler, B., Scholz, W., Fischer, L., Herrmann, H., Kulmala, M., and Hansel, A.: Accretion Product Formation from Ozonolysis and OH Radical Reaction of α-Pinene: Mechanistic Insight and the Influence of Isoprene and Ethylene, Environ. Sci. Technol., 52, 11069–11077,, 2018. 

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., and Ehn, M.: Highly Oxygenated Organic Molecules (HOM) from Gas-Phase Autoxidation Involving Peroxy Radicals: A Key Contributor to Atmospheric Aerosol, Chem. Rev., 119, 3472–3509,, 2019. 

Boucher, O., Randall, D., Artaxo, P., Bretherton, C., Feingold, G., Forster, P., Kerminen, V.-M., Kondo, Y., Liao, H., and Lohmann, U.: Clouds and aerosols, in: Climate change 2013: the physical science basis, in: Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change, Cambridge University Press, 571–657,, 2013. 

Boyd, C. M., Sanchez, J., Xu, L., Eugene, A. J., Nah, T., Tuet, W. Y., Guzman, M. I., and Ng, N. L.: Secondary organic aerosol formation from the beta-pinene + NO3 system: effect of humidity and peroxy radical fate, Atmos. Chem. Phys., 15, 7497–7522,, 2015. 

Canagaratna, M., Jayne, J., Jimenez, J., Allan, J., Alfarra, M., Zhang, Q., Onasch, T., Drewnick, F., Coe, H., and Middlebrook, A.: Chemical and microphysical characterization of ambient aerosols with the aerodyne aerosol mass spectrometer, Mass Spectrom. Rev., 26, 185–222,, 2007. 

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., and Worsnop, D. R.: Elemental ratio measurements of organic compounds using aerosol mass spectrometry: characterization, improved calibration, and implications, Atmos. Chem. Phys., 15, 253–272,, 2015. 

Caudillo, L., Rörup, B., Heinritzi, M., Marie, G., Simon, M., Wagner, A. C., Müller, T., Granzin, M., Amorim, A., Ataei, F., Baalbaki, R., Bertozzi, B., Brasseur, Z., Chiu, R., Chu, B., Dada, L., Duplissy, J., Finkenzeller, H., Gonzalez Carracedo, L., He, X. C., Hofbauer, V., Kong, W., Lamkaddam, H., Lee, C. P., Lopez, B., Mahfouz, N. G. A., Makhmutov, V., Manninen, H. E., Marten, R., Massabò, D., Mauldin, R. L., Mentler, B., Molteni, U., Onnela, A., Pfeifer, J., Philippov, M., Piedehierro, A. A., Schervish, M., Scholz, W., Schulze, B., Shen, J., Stolzenburg, D., Stozhkov, Y., Surdu, M., Tauber, C., Tham, Y. J., Tian, P., Tomé, A., Vogt, S., Wang, M., Wang, D. S., Weber, S. K., Welti, A., Yonghong, W., Yusheng, W., Zauner-Wieczorek, M., Baltensperger, U., El Haddad, I., Flagan, R. C., Hansel, A., Höhler, K., Kirkby, J., Kulmala, M., Lehtipalo, K., Möhler, O., Saathoff, H., Volkamer, R., Winkler, P. M., Donahue, N. M., Kürten, A., and Curtius, J.: Chemical composition of nanoparticles from α-pinene nucleation and the influence of isoprene and relative humidity at low temperature, Atmos. Chem. Phys., 21, 17099–17114,, 2021. 

Chhabra, P. S., Flagan, R. C., and Seinfeld, J. H.: Elemental analysis of chamber organic aerosol using an aerodyne high-resolution aerosol mass spectrometer, Atmos. Chem. Phys., 10, 4111–4131,, 2010. 

Claeys, M., Iinuma, Y., Szmigielski, R., Surratt, J. D., Blockhuys, F., Van Alsenoy, C., Böge, O., Sierau, B., Gómez-González, Y., Vermeylen, R., Van der Veken, P., Shahgholi, M., Chan, A. W. H., Herrmann, H., Seinfeld, J. H., and Maenhaut, W.: Terpenylic Acid and Related Compounds from the Oxidation of α-Pinene: Implications for New Particle Formation and Growth above Forests, Environ. Sci. Technol., 43, 6976–6982,, 2009. 

Claflin, M. S. and 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, 122, 3640–3652,, 2018. 

Claflin, M. S., Krechmer, J. E., Hu, W., Jimenez, J. L., and Ziemann, P. J.: Functional Group Composition of Secondary Organic Aerosol Formed from Ozonolysis of α-Pinene Under High VOC and Autoxidation Conditions, ACS Earth Space Chem., 2, 1196–1210,, 2018. 

Crounse, J. D., Nielsen, L. B., Jørgensen, S., Kjaergaard, H. G., and Wennberg, P. O.: Autoxidation of Organic Compounds in the Atmosphere, J. Phys. Chem. Lett., 4, 3513–3520,, 2013. 

Day, D. A., Campuzano-Jost, P., Nault, B. A., Palm, B. B., Hu, W., Guo, H., Wooldridge, P. J., Cohen, R. C., Docherty, K. S., Huffman, J. A., de Sá, S. S., Martin, S. T., and Jimenez, J. L.: A systematic re-evaluation of methods for quantification of bulk particle-phase organic nitrates using real-time aerosol mass spectrometry, Atmos. Meas. Tech., 15, 459–483,, 2022. 

DeCarlo, P. F., Kimmel, J. R., Trimborn, A., Northway, M. J., Jayne, J. T., Aiken, A. C., Gonin, M., Fuhrer, K., Horvath, T., and Docherty, K. S.: Field-deployable, high-resolution, time-of-flight aerosol mass spectrometer, Anal. chem., 78, 8281–8289,, 2006. 

Ding, X., He, Q.-F., Shen, R.-Q., Yu, Q.-Q., and Wang, X.-M.: Spatial distributions of secondary organic aerosols from isoprene, monoterpenes, β-caryophyllene, and aromatics over China during summer, J. Geophys. Res.-Atmos., 119, 11877–11891,, 2014. 

Docherty, K. S., Wu, W., Lim, Y. B., and Ziemann, P. J.: Contributions of organic peroxides to secondary aerosol formed from reactions of monoterpenes with O3, Environ. Sci. Technol., 39, 4049–4059,, 2005. 

Donahue, N. M., Kroll, J. H., Pandis, S. N., and Robinson, A. L.: A two-dimensional volatility basis set – Part 2: Diagnostics of organic-aerosol evolution, Atmos. Chem. Phys., 12, 615–634,, 2012. 

Donahue, N. M., Ortega, I. K., Chuang, W., Riipinen, I., Riccobono, F., Schobesberger, S., Dommen, J., Baltensperger, U., Kulmala, M., Worsnop, D. R., and Vehkamaki, H.: How do organic vapors contribute to new-particle formation?, Faraday Discuss., 165, 91–104,, 2013. 

Ehn, M., Kleist, E., Junninen, H., Petäjä, T., Lönn, G., Schobesberger, S., Dal Maso, M., Trimborn, A., Kulmala, M., Worsnop, D. R., Wahner, A., Wildt, J., and Mentel, T. F.: Gas phase formation of extremely oxidized pinene reaction products in chamber and ambient air, Atmos. Chem. Phys., 12, 5113–5127,, 2012. 

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., and Mentel, T. F.: A large source of low-volatility secondary organic aerosol, Nature, 506, 476–479,, 2014. 

Ehn, M., Berndt, T., Wildt, J., and Mentel, T.: Highly Oxygenated Molecules from Atmospheric Autoxidation of Hydrocarbons: A Prominent Challenge for Chemical Kinetics Studies, Int. J. Chem. Kinet., 49, 821–831,, 2017. 

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,, 2015. 

Eisele, F. L. and Tanner, D. J.: Measurement of the gas phase concentration of H2SO4 and methane sulfonic acid and estimates of H2SO4 production and loss in the atmosphere, J. Geophys. Res.-Atmos., 98, 9001–9010,, 1993. 

Farmer, D. K., Matsunaga, A., Docherty, K. S., Surratt, J. D., Seinfeld, J. H., Ziemann, P. J., and Jimenez, J. L.: Response of an aerosol mass spectrometer to organonitrates and organosulfates and implications for atmospheric chemistry, P. Natl. Acad. Sci. USA, 107, 6670–6675,, 2010. 

Griffin, R. J., Cocker III, D. R., Flagan, R. C., and Seinfeld, J. H.: Organic aerosol formation from the oxidation of biogenic hydrocarbons, J. Geophys. Res.-Atmos., 104, 3555–3567,, 1999. 

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,, 2012. 

Häkkinen, E., Zhao, J., Graeffe, F., Fauré, N., Krechmer, J., Worsnop, D., Timonen, H., Ehn, M., and Kangasluoma, J.: Online measurement of highly oxygenated compounds from organic aerosol, EGUsphere [preprint],, 2022. 

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., 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,, 2009. 

Hoffmann, T., Odum, J. R., Bowman, F., Collins, D., Klockow, D., Flagan, R. C., and Seinfeld, J. H.: Formation of Organic Aerosols from the Oxidation of Biogenic Hydrocarbons, J. Atmos. Chem., 26, 189–222,, 1997. 

Hyttinen, N., Kupiainen-Määttä, O., Rissanen, M. P., Muuronen, M., Ehn, M., and Kurtén, T.: Modeling the Charging of Highly Oxidized Cyclohexene Ozonolysis Products Using Nitrate-Based Chemical Ionization, J. Phys. Chem. A, 119, 6339–6345,, 2015. 

Hyttinen, N., Rissanen, M. P., and Kurtén, T.: Computational Comparison of Acetate and Nitrate Chemical Ionization of Highly Oxidized Cyclohexene Ozonolysis Intermediates and Products, J. Phys. Chem. A, 121, 2172–2179,, 2017. 

Hyttinen, N., Wolf, M., Rissanen, M. P., Ehn, M., Peräkylä, O., Kurtén, T., and Prisle, N. L.: Gas-to-Particle Partitioning of Cyclohexene- and α-Pinene-Derived Highly Oxygenated Dimers Evaluated Using COSMOtherm, J. Phys. Chem. A, 125, 3726–3738,, 2021. 

Iyer, S., Reiman, H., Møller, K. H., Rissanen, M. P., Kjaergaard, H. G., and Kurtén, T.: Computational Investigation of RO2+HO2 and RO2+RO2 Reactions of Monoterpene Derived First-Generation Peroxy Radicals Leading to Radical Recycling, J. Phys. Chem. A, 122, 9542–9552,, 2018. 

Iyer, S., Rissanen, M. P., Valiev, R., Barua, S., Krechmer, J. E., Thornton, J., Ehn, M., and Kurtén, T.: Molecular mechanism for rapid autoxidation in α-pinene ozonolysis, Nat. Commun., 12, 878,, 2021. 

Jayne, J. T., Leard, D. C., Zhang, X., Davidovits, P., Smith, K. A., Kolb, C. E., and Worsnop, D. R.: Development of an Aerosol Mass Spectrometer for Size and Composition Analysis of Submicron Particles, Aerosol Sci. Tech., 33, 49–70,, 2000. 

Jimenez, J., Canagaratna, M., Donahue, N., Prevot, A., Zhang, Q., Kroll, J. H., DeCarlo, P. F., Allan, J. D., Coe, H., and Ng, N.: Evolution of organic aerosols in the atmosphere, Science, 326, 1525–1529,, 2009. 

Jokinen, T., Sipilä, M., Junninen, H., Ehn, M., Lönn, G., Hakala, J., Petäjä, T., Mauldin Iii, R. L., Kulmala, M., and Worsnop, D. R.: Atmospheric sulphuric acid and neutral cluster measurements using CI-APi-TOF, Atmos. Chem. Phys., 12, 4117–4125,, 2012. 

Jokinen, T., Sipila, M., Richters, S., Kerminen, V. M., Paasonen, P., Stratmann, F., Worsnop, D., Kulmala, M., Ehn, M., Herrmann, H., and Berndt, T.: Rapid autoxidation forms highly oxidized RO2 radicals in the atmosphere, Angew. Chem., 53, 14596–14600,, 2014. 

Jokinen, T., Berndt, T., Makkonen, R., Kerminen, V. M., Junninen, H., Paasonen, P., Stratmann, F., Herrmann, H., Guenther, A. B., Worsnop, D. R., Kulmala, M., Ehn, M., and Sipila, M.: Production of extremely low volatile organic compounds from biogenic emissions: Measured yields and atmospheric implications, P. Natl. Acad. Sci. USA, 112, 7123–7128,, 2015. 

Junninen, H., Ehn, M., Petäjä, T., Luosujärvi, L., Kotiaho, T., Kostiainen, R., Rohner, U., Gonin, M., Fuhrer, K., Kulmala, M., and Worsnop, D. R.: A high-resolution mass spectrometer to measure atmospheric ion composition, Atmos. Meas. Tech., 3, 1039–1053,, 2010. 

Kahnt, A., Vermeylen, R., Iinuma, Y., Safi Shalamzari, M., Maenhaut, W., and Claeys, M.: High-molecular-weight esters in α-pinene ozonolysis secondary organic aerosol: structural characterization and mechanistic proposal for their formation from highly oxygenated molecules, Atmos. Chem. Phys., 18, 8453–8467,, 2018. 

Kalberer, M., Paulsen, D., Sax, M., Steinbacher, M., Dommen, J., Prevot, A. S. H., Fisseha, R., Weingartner, E., Frankevich, V., Zenobi, R., and Baltensperger, U.: Identification of Polymers as Major Components of Atmospheric Organic Aerosols, Science, 303, 1659–1662,, 2004. 

Kang, E., Root, M. J., Toohey, D. W., and Brune, W. H.: Introducing the concept of Potential Aerosol Mass (PAM), Atmos. Chem. Phys., 7, 5727–5744,, 2007. 

Kerdouci, J., Picquet-Varrault, B., and Doussin, J.-F.: Prediction of Rate Constants for Gas-Phase Reactions of Nitrate Radical with Organic Compounds: A New Structure–Activity Relationship, Chem. Phys. Chem., 11, 3909–3920,, 2010. 

Kirkby, J., Duplissy, J., Sengupta, K., Frege, C., Gordon, H., Williamson, C., Heinritzi, M., Simon, M., Yan, C., Almeida, J., Trostl, J., Nieminen, T., Ortega, I. K., Wagner, R., Adamov, A., Amorim, A., Bernhammer, A. K., Bianchi, F., Breitenlechner, M., Brilke, S., Chen, X., Craven, J., Dias, A., Ehrhart, S., Flagan, R. C., Franchin, A., Fuchs, C., Guida, R., Hakala, J., Hoyle, C. R., Jokinen, T., Junninen, H., Kangasluoma, J., Kim, J., Krapf, M., Kurten, A., Laaksonen, A., Lehtipalo, K., Makhmutov, V., Mathot, S., Molteni, U., Onnela, A., Perakyla, O., Piel, F., Petaja, T., Praplan, A. P., Pringle, K., Rap, A., Richards, N. A., Riipinen, I., Rissanen, M. P., Rondo, L., Sarnela, N., Schobesberger, S., Scott, C. E., Seinfeld, J. H., Sipila, M., Steiner, G., Stozhkov, Y., Stratmann, F., Tome, A., Virtanen, A., Vogel, A. L., Wagner, A. C., Wagner, P. E., Weingartner, E., Wimmer, D., Winkler, P. M., Ye, P., Zhang, X., Hansel, A., Dommen, J., Donahue, N. M., Worsnop, D. R., Baltensperger, U., Kulmala, M., Carslaw, K. S., and Curtius, J.: Ion-induced nucleation of pure biogenic particles, Nature, 533, 521–526,, 2016. 

Krapf, M., El Haddad, I., Bruns, E. A., Molteni, U., Daellenbach, K. R., Prévôt, A. S. H., Baltensperger, U., and Dommen, J.: Labile Peroxides in Secondary Organic Aerosol, Chem, 1, 603–616,, 2016. 

Kristensen, K., Cui, T., Zhang, H., Gold, A., Glasius, M., and Surratt, J. D.: Dimers in α-pinene secondary organic aerosol: effect of hydroxyl radical, ozone, relative humidity and aerosol acidity, Atmos. Chem. Phys., 14, 4201–4218,, 2014. 

Kristensen, K., Watne, Å. K., Hammes, J., Lutz, A., Petäjä, T., Hallquist, M., Bilde, M., and Glasius, M.: High-Molecular Weight Dimer Esters Are Major Products in Aerosols from α-Pinene Ozonolysis and the Boreal Forest, Environ. Sci. Technol. Lett., 3, 280–285,, 2016. 

Kristensen, K., Jensen, L. N., Quéléver, L. L. J., Christiansen, S., Rosati, B., Elm, J., Teiwes, R., Pedersen, H. B., Glasius, M., Ehn, M., and Bilde, M.: The Aarhus Chamber Campaign on Highly Oxygenated Organic Molecules and Aerosols (ACCHA): particle formation, organic acids, and dimer esters from α-pinene ozonolysis at different temperatures, Atmos. Chem. Phys., 20, 12549–12567,, 2020. 

Kulmala, M., Petäjä, T., Ehn, M., Thornton, J., Sipilä, M., Worsnop, D. R., and Kerminen, V.-M.: Chemistry of Atmospheric Nucleation: On the Recent Advances on Precursor Characterization and Atmospheric Cluster Composition in Connection with Atmospheric New Particle Formation, Annu. Rev. Phys. Chem., 65, 21-37,, 2014. 

Kurtén, T., Tiusanen, K., Roldin, P., Rissanen, M., Luy, J. N., Boy, M., Ehn, M., and Donahue, N.: alpha-Pinene Autoxidation Products May Not Have Extremely Low Saturation Vapor Pressures Despite High O:C Ratios, J. Phys. Chem. A, 120, 2569–2582,, 2016. 

Kurtén, T., Møller, K. H., Nguyen, T. B., Schwantes, R. H., Misztal, P. K., Su, L., Wennberg, P. O., Fry, J. L., and Kjaergaard, H. G.: Alkoxy Radical Bond Scissions Explain the Anomalously Low Secondary Organic Aerosol and Organonitrate Yields From α-Pinene + NO3, J. Phys. Chem. Lett., 8, 2826–2834,, 2017. 

Lambe, A. T., Ahern, A. T., Williams, L. R., Slowik, J. G., Wong, J. P. S., Abbatt, J. P. D., Brune, W. H., Ng, N. L., Wright, J. P., Croasdale, D. R., Worsnop, D. R., Davidovits, P., and Onasch, T. B.: Characterization of aerosol photooxidation flow reactors: heterogeneous oxidation, secondary organic aerosol formation and cloud condensation nuclei activity measurements, Atmos. Meas. Tech., 4, 445–461,, 2011. 

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., and Thornton, J. A.: Highly functionalized organic nitrates in the southeast United States: Contribution to secondary organic aerosol and reactive nitrogen budgets, P. Natl. Acad. Sci. USA, 113, 1516–1521,, 2016. 

Lee, C. P., Surdu, M., Bell, D. M., Dommen, J., Xiao, M., Zhou, X., Baccarini, A., Giannoukos, S., Wehrle, G., Schneider, P. A., Prevot, A. S. H., Slowik, J. G., Lamkaddam, H., Wang, D., Baltensperger, U., and El Haddad, I.: High-frequency gaseous and particulate chemical characterization using extractive electrospray ionization mass spectrometry (Dual-Phase-EESI-TOF), Atmos. Meas. Tech., 15, 3747–3760,, 2022. 

Lopez-Hilfiker, F. D., Mohr, C., Ehn, M., Rubach, F., Kleist, E., Wildt, J., Mentel, T. 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,, 2014. 

Lopez-Hilfiker, F. D., Mohr, C., Ehn, M., Rubach, F., Kleist, E., Wildt, J., Mentel, T. F., Carrasquillo, A. J., Daumit, K. E., Hunter, J. F., Kroll, J. H., Worsnop, D. R., and Thornton, J. A.: Phase partitioning and volatility of secondary organic aerosol components formed from α-pinene ozonolysis and OH oxidation: the importance of accretion products and other low volatility compounds, Atmos. Chem. Phys., 15, 776–7776,, 2015. 

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,, 2019. 

Mauderly, J. L. and Chow, J. C.: Health effects of organic aerosols, Inhalat. Toxicol., 20, 257–288,, 2008. 

McFiggans, G., Mentel, T. F., Wildt, J., Pullinen, I., Kang, S., Kleist, E., Schmitt, S., Springer, M., Tillmann, R., Wu, C., Zhao, D., Hallquist, M., Faxon, C., Le Breton, M., Hallquist, Å. M., Simpson, D., Bergström, R., Jenkin, M. E., Ehn, M., Thornton, J. A., Alfarra, M. R., Bannan, T. J., Percival, C. J., Priestley, M., Topping, D., and Kiendler-Scharr, A.: Secondary organic aerosol reduced by mixture of atmospheric vapours, Nature, 565, 587–593,, 2019. 

Mentel, T. F., Springer, M., Ehn, M., Kleist, E., Pullinen, I., Kurtén, T., Rissanen, M., Wahner, A., and 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., 15, 6745–6765,, 2015. 

Molteni, U., Simon, M., Heinritzi, M., Hoyle, C. R., Bernhammer, A.-K., Bianchi, F., Breitenlechner, M., Brilke, S., Dias, A., Duplissy, J., Frege, C., Gordon, H., Heyn, C., Jokinen, T., Kürten, A., Lehtipalo, K., Makhmutov, V., Petäjä, T., Pieber, S. M., Praplan, A. P., Schobesberger, S., Steiner, G., Stozhkov, Y., Tomé, A., Tröstl, J., Wagner, A. C., Wagner, R., Williamson, C., Yan, C., Baltensperger, U., Curtius, J., Donahue, N. M., Hansel, A., Kirkby, J., Kulmala, M., Worsnop, D. R., and Dommen, J.: Formation of Highly Oxygenated Organic Molecules from α-Pinene Ozonolysis: Chemical Characteristics, Mechanism, and Kinetic Model Development, ACS Earth Space Chem., 3, 873–883,, 2019. 

Müller, L., Reinnig, M.-C., Hayen, H., and Hoffmann, T.: Characterization of oligomeric compounds in secondary organic aerosol using liquid chromatography coupled to electrospray ionization Fourier transform ion cyclotron resonance mass spectrometry, Rapid Commun. Mass Spectrom., 23, 971–979,, 2009. 

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,, 2017. 

Mutzel, A., Poulain, L., Berndt, T., Iinuma, Y., Rodigast, M., Böge, O., Richters, S., Spindler, G., Sipilä, M., Jokinen, T., Kulmala, M., and Herrmann, H.: Highly Oxidized Multifunctional Organic Compounds Observed in Tropospheric Particles: A Field and Laboratory Study, Environ. Sci. Technol., 49, 7754–7761,, 2015. 

Nah, T., Sanchez, J., Boyd, C. M., and Ng, N. L.: Photochemical Aging of α-pinene and β-pinene Secondary Organic Aerosol formed from Nitrate Radical Oxidation, Environ. Sci. Technol., 50, 222–231,, 2016. 

Orlando, J. J. and Tyndall, G. S.: Laboratory studies of organic peroxy radical chemistry: an overview with emphasis on recent issues of atmospheric significance, Chem. Soc. Rev., 41, 6294–6317,, 2012. 

Peräkylä, O., Riva, M., Heikkinen, L., Quéléver, L., Roldin, P., and Ehn, M.: Experimental investigation into the volatilities of highly oxygenated organic molecules (HOMs), Atmos. Chem. Phys., 20, 649–669,, 2020. 

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, Sci. Adv., 6, eaax8922,, 2020. 

Presto, A. A., Huff Hartz, K. E., and Donahue, N. M.: Secondary Organic Aerosol Production from Terpene Ozonolysis. 2. Effect of NOx Concentration, Environ. Sci. Technol., 39, 7046–7054,, 2005. 

Pullinen, I., Schmitt, S., Kang, S., Sarrafzadeh, M., Schlag, P., Andres, S., Kleist, E., Mentel, T. F., Rohrer, F., Springer, M., Tillmann, R., Wildt, J., Wu, C., Zhao, D., Wahner, A., and Kiendler-Scharr, A.: Impact of NOx on secondary organic aerosol (SOA) formation from α-pinene andβ-pinene photooxidation: the role of highly oxygenated organic nitrates, Atmos. Chem. Phys., 20, 10125–10147,, 2020. 

Reinnig, M. C., Warnke, J., and Hoffmann, T.: Identification of organic hydroperoxides and hydroperoxy acids in secondary organic aerosol formed during the ozonolysis of different monoterpenes and sesquiterpenes by on-line analysis using atmospheric pressure chemical ionization ion trap mass spectrometry, Rapid Commun. Mass Spectrom., 23, 1735–1741,, 2009. 

Rissanen, M. P.: NO2 Suppression of Autoxidation–Inhibition of Gas-Phase Highly Oxidized Dimer Product Formation, ACS Earth Space Chem., 2, 1211–1219,, 2018. 

Rissanen, M. P., Kurten, T., Sipila, M., Thornton, J. A., Kangasluoma, J., Sarnela, N., Junninen, H., Jorgensen, S., Schallhart, S., Kajos, M. K., Taipale, R., Springer, M., Mentel, T. F., Ruuskanen, T., Petaja, T., Worsnop, D. R., Kjaergaard, H. G., and Ehn, M.: The formation of highly oxidized multifunctional products in the ozonolysis of cyclohexene, J. Am. Chem. Soc., 136, 15596–15606,, 2014. 

Riva, M., Rantala, P., Krechmer, J. E., Peräkylä, O., Zhang, Y., Heikkinen, L., Garmash, O., Yan, C., Kulmala, M., Worsnop, D., and Ehn, M.: Evaluating the performance of five different chemical ionization techniques for detecting gaseous oxygenated organic species, Atmos. Meas. Tech., 12, 2403–2421,, 2019. 

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,, 2017. 

Takeuchi, M. and 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., 19, 12749–12766,, 2019. 

Vereecken, L., Glowacki, D. R., and Pilling, M. J.: Theoretical Chemical Kinetics in Tropospheric Chemistry: Methodologies and Applications, Chem. Rev., 115, 4063–4114,, 2015. 

Wagner, A. C., Bergen, A., Brilke, S., Fuchs, C., Ernst, M., Hoker, J., Heinritzi, M., Simon, M., Bühner, B., Curtius, J., and Kürten, A.: Size-resolved online chemical analysis of nanoaerosol particles: a thermal desorption differential mobility analyzer coupled to a chemical ionization time-of-flight mass spectrometer, Atmos. Meas. Tech., 11, 5489–5506,, 2018. 

Wang, Y., Riva, M., Xie, H., Heikkinen, L., Schallhart, S., Zha, Q., Yan, C., He, X.-C., Peräkylä, O., and Ehn, M.: Formation of highly oxygenated organic molecules from chlorine-atom-initiated oxidation of α-pinene, Atmos. Chem. Phys., 20, 5145–5155,, 2020. 

Wang, Z., Popolan-Vaida, D. M., Chen, B., Moshammer, K., Mohamed, S. Y., Wang, H., Sioud, S., Raji, M. A., Kohse-Höinghaus, K., Hansen, N., Dagaut, P., Leone, S. R., and Sarathy, S. M.: Unraveling the structure and chemical mechanisms of highly oxygenated intermediates in oxidation of organic compounds, P. Natl. Acad. Sci. USA, 114, 13102–13107,, 2017. 

Yasmeen, F., Vermeylen, R., Szmigielski, R., Iinuma, Y., Böge, O., Herrmann, H., Maenhaut, W., and Claeys, M.: Terpenylic acid and related compounds: precursors for dimers in secondary organic aerosol from the ozonolysis of α- and β-pinene, Atmos. Chem. Phys., 10, 9383–9392,, 2010. 

Yatavelli, R. L. N., Lopez-Hilfiker, F., Wargo, J. D., Kimmel, J. R., Cubison, M. J., Bertram, T. H., Jimenez, J. L., Gonin, M., Worsnop, D. R., and Thornton, J. A.: A Chemical Ionization High-Resolution Time-of-Flight Mass Spectrometer Coupled to a Micro Orifice Volatilization Impactor (MOVI-HRToF-CIMS) for Analysis of Gas and Particle-Phase Organic Species, Aerosol Sci. Tech., 46, 1313–1327,, 2012. 

Yatavelli, R. L. N., Mohr, C., Stark, H., Day, D. A., Thompson, S. L., Lopez-Hilfiker, F. D., Campuzano-Jost, P., Palm, B. B., Vogel, A. L., Hoffmann, T., Heikkinen, L., Aijala, M., Ng, N. L., Kimmel, J. R., Canagaratna, M. R., Ehn, M., Junninen, H., Cubison, M. J., Petaja, T., Kulmala, M., Jayne, J. T., Worsnop, D. R., and Jimenez, J. L.: Estimating the contribution of organic acids to northern hemispheric continental organic aerosol, Geophys. Res. Lett., 42, 6084–6090,, 2015.  

Zhang, H., Yee, L. D., Lee, B. H., Curtis, M. P., Worton, D. R., Isaacman-VanWertz, G., Offenberg, J. H., Lewandowski, M., Kleindienst, T. E., Beaver, M. R., Holder, A. L., Lonneman, W. A., Docherty, K. S., Jaoui, M., Pye, H. O. T., Hu, W., Day, D. A., Campuzano-Jost, P., Jimenez, J. L., Guo, H., Weber, R. J., de Gouw, J., Koss, A. R., Edgerton, E. S., Brune, W., Mohr, C., Lopez-Hilfiker, F. D., Lutz, A., Kreisberg, N. M., Spielman, S. R., Hering, S. V., Wilson, K. R., Thornton, J. A., and Goldstein, A. H.: Monoterpenes are the largest source of summertime organic aerosol in the southeastern United States, P. Natl. Acad. Sci. USA, 115, 2038–2043,, 2018. 

Zhang, X., McVay, R. C., Huang, D. D., Dalleska, N. F., Aumont, B., Flagan, R. C., and Seinfeld, J. H.: Formation and evolution of molecular products in α-pinene secondary organic aerosol, P. Natl. Acad. Sci. USA, 112, 14168–14173,, 2015. 

Zhang, X., Lambe, A. T., Upshur, M. A., Brooks, W. A., Gray Bé, A., Thomson, R. J., Geiger, F. M., Surratt, J. D., Zhang, Z., Gold, A., Graf, S., Cubison, M. J., Groessl, M., Jayne, J. T., Worsnop, D. R., and Canagaratna, M. R.: Highly Oxygenated Multifunctional Compounds in α-Pinene Secondary Organic Aerosol, Environ. Sci. Technol., 51, 5932–5940,, 2017. 

Zhao, D., Schmitt, S. H., Wang, M., Acir, I. H., Tillmann, R., Tan, Z., Novelli, A., Fuchs, H., Pullinen, I., Wegener, R., Rohrer, F., Wildt, J., Kiendler-Scharr, A., Wahner, A., and Mentel, T. F.: Effects of NOx and SO2 on the secondary organic aerosol formation from photooxidation of α-pinene and limonene, Atmos. Chem. Phys., 18, 1611–1628,, 2018. 

Zhao, Y., Thornton, J. A., and Pye, H. O. T.: Quantitative constraints on autoxidation and dimer formation from direct probing of monoterpene-derived peroxy radical chemistry, P. Natl. Acad. Sci. USA, 115, 12142–12147,, 2018. 

Short summary
Based on the combined measurements of gas- and particle-phase highly oxygenated organic molecules (HOMs) from α-pinene ozonolysis, enhancement of dimers in particles was observed. We conducted experiments wherein the dimer to monomer (D / M) ratios of HOMs in the gas phase were modified (adding CO / NO) to investigate the effects of the corresponding D / M ratios in the particles. These results are important for a better understanding of secondary organic aerosol formation in the atmosphere.
Final-revised paper