Biomass-burning-derived particles from a wide variety of fuels – Part 2: Effects of photochemical aging on particle optical and chemical properties

Particles in smoke emitted from biomass combustion have a large impact on global climate and urban air quality. There is limited understanding of how particle optical properties – especially the contributions of black carbon (BC) and brown carbon (BrC) – evolve with photochemical aging of smoke. We analyze the evolution of the optical properties and chemical composition of particles produced from combustion of a wide variety of biomass fuels, largely from the western United States. The smoke is photochemically aged in a reaction chamber over atmospheric-equivalent timescales ranging from 0.25 to 8 d. Various aerosol optical properties (e.g., the single-scatter albedo, the wavelength dependence of absorption, and the BC mass absorption coefficient, MACBC) evolved with photochemical aging, with the specific evolution dependent on the initial particle properties and conditions. The impact of coatings on BC absorption (the so-called lensing effect) was small, even after photochemical aging. The initial evolution of the BrC absorptivity (MACBrC) varied between individual burns but decreased consistently at longer aging times; the wavelength dependence of the BrC absorption generally increased with aging. The observed changes to BrC properties result from a combination of secondary organic aerosol (SOA) production and heterogeneous oxidation of primary and secondary OA mass, with SOA production being the major driver of the changes. The SOA properties varied with time, reflecting both formation from precursors having a range of lifetimes with respect to OH and the evolving photochemical environment within the chamber. Although the absorptivity of BrC generally decreases with aging, the dilution-corrected absorption may actually increase from the production of SOA. These experimental results provide context for the interpretation of ambient observations of the evolution of particle optical properties in biomass-combustion-derived smoke plumes. Published by Copernicus Publications on behalf of the European Geosciences Union. 8512 C. D. Cappa et al.: Biomass-burning-derived particles from a wide variety of fuels – Part 2

Abstract. Particles in smoke emitted from biomass combustion have a large impact on global climate and urban air quality. There is limited understanding of how particle optical properties -especially the contributions of black carbon (BC) and brown carbon (BrC) -evolve with photochemical aging of smoke. We analyze the evolution of the optical properties and chemical composition of particles produced from combustion of a wide variety of biomass fuels, largely from the western United States. The smoke is photochemically aged in a reaction chamber over atmospheric-equivalent timescales ranging from 0.25 to 8 d. Various aerosol optical properties (e.g., the single-scatter albedo, the wavelength dependence of absorption, and the BC mass absorption coefficient, MAC BC ) evolved with photochemical aging, with the specific evolution dependent on the initial particle properties and conditions. The impact of coatings on BC absorption (the so-called lensing effect) was small, even after photochemical aging. The initial evolution of the BrC absorptivity (MAC BrC ) varied between individual burns but decreased consistently at longer aging times; the wavelength depen-dence of the BrC absorption generally increased with aging. The observed changes to BrC properties result from a combination of secondary organic aerosol (SOA) production and heterogeneous oxidation of primary and secondary OA mass, with SOA production being the major driver of the changes. The SOA properties varied with time, reflecting both formation from precursors having a range of lifetimes with respect to OH and the evolving photochemical environment within the chamber. Although the absorptivity of BrC generally decreases with aging, the dilution-corrected absorption may actually increase from the production of SOA. These experimental results provide context for the interpretation of ambient observations of the evolution of particle optical properties in biomass-combustion-derived smoke plumes.

Introduction
Open and contained biomass combustion contributes substantial amounts of particulate matter to the atmosphere (Bond et al., 2004). The emitted particles have a strong influence on global climate by scattering and absorbing solar radiation and impacting cloud properties and stratospheric water content (Penner et al., 1992;Sherwood, 2002;Jacobson, 2014). Biomass-burning-derived particles (BB particles, for short) also have substantial negative impacts on human health globally (Lelieveld et al., 2015), especially when produced as a result of indoor combustion associated with residential cooking and heating. In some parts of the world the frequency and severity of uncontrolled fires is rising and projected to become worse in the future as a consequence of climate change (Dale et al., 2001;Stephens et al., 2013), with effects already being seen in some regions (McClure and Jaffe, 2018).
Particles produced from biomass burning are primarily composed of organic material and black carbon (Andreae and Merlet, 2001). The relative contribution of organic aerosol (OA) and black carbon (BC) depends on the burn conditions, which are strongly related to the fuel type and other environmental factors (McMeeking et al., 2009;McClure et al., 2020). The chemical, optical, and physical properties of freshly emitted BB particles produced from burning of various biomass fuel types under various conditions are reasonably well studied (e.g., Lewis et al., 2008;McMeeking et al., 2009;Levin et al., 2010;Cheng et al., 2016;Fortner et al., 2018;McClure et al., 2020). Such measurements have established that some fraction of the emitted OA is light absorbing, with the absorptivity dependent upon the burn conditions (Saleh et al., 2014). Light-absorbing OA is commonly referred to as brown carbon (BrC). Compared to BC, brown carbon is generally less absorbing and exhibits a much stronger wavelength dependence (Kirchstetter et al., 2004;Andreae and Gelencsér, 2006). As such, the importance of BrC to light absorption tends to increase as wavelength decreases.
The influence of atmospheric processing on the properties of biomass combustion smoke has received less attention, especially in the context of how aging influences BB particle optical properties. (Here, we use "smoke" to indicate the mixture of particles and gases emitted from biomass combustion.) Understanding how BB particles evolve over time is key to establishing their atmospheric impacts (Wang et al., 2018). Field observations of the effects of photochemical aging on BB particle optical properties, and in particular light absorption, are sparse. Forrister et al. (2015) observed that absolute absorption by water-soluble BrC decreased over time within a biomass-burning plume, with a decay time constant of about a day. Wang et al. (2016) observed that the BrC absorptivity (as opposed to the absolute absorption) decreased with photochemical age, with a similar time constant as reported by Forrister et al. (2015). However, both stud-ies suggest that there is some fraction of the BrC that is more persistent and less subject to photochemical degradation, and Zhang et al. (2017) found no decrease in BrC absorption with age for particles in convective outflow. Laboratory measurements can help provide the mechanistic understanding necessary to comprehensively interpret the field observations. Most laboratory studies investigating photochemical aging effects on optical properties, and in particular light absorption, of BB particles have done so for only a small number of individual fuel types or burn conditions and often for particles alone rather than smoke (e.g., Saleh et al., 2013;Sumlin et al., 2017;Tasoglou et al., 2017;Wong et al., 2017;Kumar et al., 2018). Thus, while these studies have proven insightful, the limited number of fuels and conditions considered makes extending the observations to the atmosphere thus far challenging.
In this study, we examine how the optical properties of BB particles evolve as a result of OH-radical-dominated photochemical aging for smoke derived from combustion of a multitude of fuel types and spanning a wide range of burn conditions. We characterize the influence of photochemical aging on optical properties for a substantially greater number of fuel types than have been reported previously in the literature for burn conditions ranging from mostly flaming to entirely smoldering. We access aging timescales ranging from a fraction of a day to many days and characterize the continuous evolution of the particle properties. We show that the BB particle optical properties evolve with photochemical oxidation, linked to both chemical evolution of the primary particles and production of secondary organic aerosol. We characterize and quantify this behavior, developing a generalizable model for the evolution of brown carbon properties in wildfire plumes.

Campaign overview and sampling strategy
The Fire Influence on Regional to Global Environments and Air Quality Experiment (FIREX-AQ) lab campaign took place at the Missoula Fire Sciences Laboratory in November 2016(NOAA, 2013. A full description of the sampling strategy and methods, including descriptions of instruments used, for our study is provided in Lim et al. (2019) and McClure et al. (2020). Only a short description is provided here. A wide variety of fuels (Table S1 in the Supplement) were combusted under realistic conditions in a large combustion chamber (ca. 12 m × 12 m × 19 m). Fuels included bear grass, rice straw, chaparral (chamise and manzanita), juniper, sagebrush, canopy, litter and mixed components from soft woods (fir, pine, spruce), rotten logs, peat, and dung. Data from the FIREX lab study are available via the NOAA website (https://www.esrl.noaa.gov/csd/projects/ firex/firelab/; last access: 24 January 2020), with data specific to this work also archived as Cappa et al. (2019a).
The particle and gas emissions from individual stack burns were injected into a 0.15 m 3 photochemical reaction chamber (the mini chamber). A burn typically lasted about 10-20 min. Smoke was transferred from the burn room to the adjacent room housing the mini chamber and associated instrumentation through a 30 m long high-velocity community inlet. The residence time in the community inlet was determined as < 2 s. Smoke from the community inlet was subsampled into the mini chamber through a PM 1 cyclone using an ejector diluter. There were some losses of particles and gases during transfer. However, comparison between the volatile organic compound (VOC) concentrations measured prior to sampling through the community inlet and from the mini chamber prior to photooxidation demonstrates losses were relatively minor (< 8 % per volatility bin, across the entire measured VOC distribution) and should not substantially impact the results here Lim et al., 2019).

The mini chamber
Prior to each burn, the chamber was flushed with clean air with RH ranging from 25 % to 40 %. Smoke was sampled into the mini chamber across an entire burn or until shortly after the concentration in the mini chamber reached maximum. An instrument suite continuously sampled air from the mini chamber (see below). Clean makeup air added from a zero-air generator (Teledyne 701H) ensured the total inflow (sample + makeup air) equaled the air being sampled out of the chamber. The actual flow rate out of the chamber varied slightly between experiments dependent upon the exact instrument suite. Given the mini chamber volume and the typical flow rates, the net dilution from the community inlet was about a factor of 7.
Details of the mini chamber and its operation are provided in Lim et al. (2019). The FIREX mini chamber operated in semibatch mode, where unoxidized smoke-laden air is first sampled into the mini chamber. After the sampling period, a clean airflow replaces the sample flow, maintaining the size of the bag over time. Oxidation is initiated by turning on one 254 nm UV light. Externally generated ozone added at 50-100 ppb serves to initiate production of OH radicals via generation of O( 1 D). The concentrations of gases and particles continuously decreased owing to dilution by clean air and wall losses. The observed decay rate of acetonitrile (ACN) provides the dilution rate (see Sect. 2.3); gases that are substantially more sticky than ACN may be lost at a faster rate. The ACN loss rate, characterized as −d log[ACN]/dt, was around 0.024 min −1 , consistent with the gas flow rates. The particle loss rate was greater owing to additional losses of particles to the walls of the chamber. The general particle mass loss rate was −d log[particles]/dt ∼ 0.038 min −1 . However, for BC-rich particles the loss rate was initially en-hanced when the lights were turned on (discussed further below). OH exposures were determined from the dilutioncorrected decay of deuterated n-butanol (D9). These are converted to an equivalent time-evolving photochemical age (t OH ) assuming [OH] = 1.5 × 10 6 molecules cm −3 . Thet OH ranged from 0.25 to about 8 d of equivalent aging. OH concentrations determined for real-world biomass burning plumes may be higher than assumed here (Akagi et al., 2012), and thus aging may happen on shorter timescales. For the model calculations in Sect. 3.2.1, the time-evolving OH exposures were converted to equivalent OH concentrations based on the time since the lights were turned on. The n-butanol (D9) measurements were available for only about half of the individual burn experiments owing to data availability limitations of the VOC measurements. While there is some experiment-to-experiment variability in thet OH values accessed, the relationship between experiment time andt OH is reasonably consistent. Thus, we use the average behavior to estimate the photochemical ages for experiments lacking direct measurement.
As discussed in Coggon et al. (2019), the conditions of the mini chamber do not perfectly represent the photochemical conditions of the atmosphere. The use of the 254 nm UV lights enhances photolysis of a small number of select nonmethane organic gases (NMOGs), especially furfural. In contrast, photolysis of NO 2 is likely substantially slower than in the atmosphere. This impacts the time evolution of the NO/NO 2 ratio and consequently radical reactions (e.g., RO 2 + NO) and NO x loss processes. The influence of photobleaching of BrC is likely underestimated relative to the atmosphere as the actual exposure time (tens of minutes) is much shorter than the equivalent photochemical age (many days). Overall, the photochemical environment in the mini chamber emphasizes OH-driven oxidation under initially high NO x conditions that rapidly shift towards low-NO x conditions .

Instrumentation
The suite of instruments sampling from the mini chamber are listed in Table S2 and further details of instrument operation and uncertainties are provided in McClure et al. (2020), Lim et al. (2019), and Coggon et al. (2019). In brief, particlephase instruments sampled alternatingly through a two-stage thermodenuder that operated at 150 and 250 • C with a residence time of ∼ 5 s. The cycle rate between ambient and thermodenuder sampling was 2 min. The ambient (bypass) line on the thermodenuder was lined with charcoal cloth to remove excess NMOG, O 3 , and NO 2 that might otherwise interfere with the measurements. Light absorption and extinction coefficients (b abs and b ext , respectively) were measured at 405 and 532 nm using the UC Davis cavity ringdown photoacoustic spectrometer (CRD-PAS) and at 781 nm using a DMT photoacoustic soot spectrometer (PASS-3). Estimated uncertainties for the absorption measurements 8514 C. D. Cappa et al.: Biomass-burning-derived particles from a wide variety of fuels -Part 2 were 8 %, 5 %, and 10 % at 405, 532, and 781 nm, respectively. Particle size distributions were measured using a scanning electrical mobility spectrometer (SEMS;model 2002, Brechtel Mfg., Inc.). The overall concentration and composition of submicron nonrefractory particulate matter (NR-PM 1 ) were measured using a high-resolution time-of-flight aerosol mass spectrometer (HR-AMS; Aerodyne Research, Inc.). The concentration and composition of refractory-BCcontaining particles were characterized using a soot particle aerosol mass spectrometer (SP-AMS; Aerodyne Research, Inc.); the SP-AMS was operated with only laser vaporization of particles such that it was sensitive to only those particles containing refractory black carbon (rBC). Refractory black carbon concentrations and size distributions for volume-equivalent diameters from 90 to 350 nm were quantitatively measured using a single-particle soot photometer (SP2; DMT). Refractory BC outside of this size window was accounted for through multimodal fitting of the observed mass-weighted size distributions. The estimated uncertainty in the rBC concentration is 30 %. Gas-phase instruments sampled directly from the mini chamber through Teflon sampling lines. These included a proton-transferreaction time-of-flight mass spectrometer (PTR-ToF-MS) to characterize primary organic gases (Yuan et al., 2017), an I − chemical ionization mass spectrometer to characterize various gas-phase organic oxidation products, an ozone monitor (2B Technologies, model 202), a CO monitor (Teledyne, model T300), and a CO 2 monitor (LI-COR, LI-840A).

Brown carbon, coatings, and particle classification
Mass absorption coefficients, referenced to BC, are calculated as where b abs is the absorption coefficient (Mm −1 ) and [BC] is the concentration of refractory black carbon (µg m −3 ). The observed MAC BC may include contributions to absorption from both the BrC (the BrC enhancement, E abs,BrC ) and from the so-called lensing effect that can occur when nonabsorbing coatings mix with BC (the coating-induced enhancement, E abs,coat ) . The observable absorption enhancement is characterized as . The MAC BC,pure equals 11.8 ± 1.2 m 2 g −1 (405 nm), 8.8 ± 0.9 m 2 g −1 (532 nm), and 5.5 ± 0.6 m 2 g −1 (781 nm). We assume these reference values are applicable to all burns, consistent with the negligible dependence of the primary particle MAC BC,781 nm on the coating-to-BC mass ratio (R coat-rBC ) (McClure et al., 2020) and the lack of size dependence of the MAC BC,pure measured for uncoated BC particles produced from a laboratory flame (Forestieri et al., 2018). The use of a campaign-specific value helps to mitigate instrumental uncertainties in determining E abs (Cappa et al., 2019b). We observe limited change in the E abs,781 nm with photochemical aging here, with E abs,781 nm for aged particles averaging 1.19 for R coat-rBC < 9 (Fig. S2). The E abs,781 nm (and MAC BC,781 nm ) only increases notably (by more than 10 %) when R coat-rBC > 9, while theory predicts the MAC BC,781 nm should increase by this amount for individual particles when R coat-rBC > 1 (Fuller et al., 1999). Other laboratory experiments, often performed using monodisperse BC seed particles, have observed substantial coating-induced enhancements and a dependence on the R coat-rBC (e.g., Cross et al., 2010;Shiraiwa et al., 2010;Metcalf et al., 2013;You et al., 2016). We suggest that the small E abs,coat for photochemically aged biomass combustion particles results from three phenomena: (i) condensation occurring onto a polydisperse rBC distribution, leading to some particles having very thick coatings and some quite thin, yielding a large average R coat-rBC yet small enhancement (Fierce et al., 2016(Fierce et al., , 2020; (ii) the coated biomassburning-derived rBC particles not having a core-shell morphology and reduced E abs,coat (Helgestad, 2016;Liu et al., 2017); and (iii) weak absorption by BrC at 781 nm by both internally and externally mixed BrC that becomes notable only when the total [OA] greatly exceeds [BC] (McClure et al., 2020). This is supported by the comparably much stronger relationship for photochemically aged particles between MAC BC,781 nm and the [OA]/[rBC] ratio than with the R coat-rBC (Fig. S2). This suggests that the majority of the variability in the MAC BC,781 nm derives from varying contributions of BrC, rather than in E abs,coat , and that E abs,coat is near unity.
The wavelength-specific BrC absorption (b abs,BrC ) is estimated as b abs,BrC = b abs,obs − MAC BC,pure · [rBC] · E abs,coat . (3) Given the above discussion and the complementary discussion in McClure et al. (2020), we assume E abs,coat is unity, with the derived b abs,BrC an upper limit. A lower limit for b abs,BrC can be obtained using an empirical E abs,coat versus R BC-coat relationship. For the aged particles, the average upper-limit b abs,BrC values exceed the lower limit b abs,BrC values by 11 (±9) % at 405 nm and 29 (±16) % at 532 nm. The brown-carbon-specific mass absorption coeffi- where λ 1 and λ 2 indicate two different measurement wavelengths. The AAE can be calculated based on the total absorption or just for BrC, with the latter designated as AAE BrC . The single-scatter albedo (SSA) characterizes the fraction of light extinction attributable to scattering:  (2020), the classifications relate somewhat to the burn-average modified combustion efficiency (MCE), which characterizes the burn efficiency, with class 1 generally deriving from more efficient, flaming burns having higher MCE and class 6 from more less efficient, smoldering burns having lower MCE. The average dependence of the various aerosol properties on photochemical age is determined for each SSA class. Grouping experiments by SSA classification are justified given the substantial variability in the primary particle properties between individual burns. The focus on average behavior increases robustness of the resulting interpretation as sensitivity to experiment-by-experiment differences (e.g., length of experiment, initial concentration, amount of fuel consumed) is reduced.

Results and discussion
3.1 Observations of the influence of photochemical aging on optical properties

Total particles (black + brown carbon)
The suite of intensive optical (e.g., SSA, MAC, AAE) and chemical and physical properties (e.g., [OA]/[rBC], R coat-rBC ) vary with photochemical aging; the average behavior for each particle class is shown in Fig. 1 and the experiment-specific behavior within each class in Figs. S3 through S8. The majority of the mass formed is OA, with minor contributions from inorganic species. A detailed assessment of secondary organic aerosol (SOA) formation is provided by Lim et al. (2019).
The changes observed for the lower-number (more BCrich) particle classes are typically more pronounced than for the higher-number (more OA-rich) particle classes. For example, the class 1 SSA 405 nm increases from 0.3 to 0.7 and the AAE 405-532 from 1.4 to 3.5 with aging, while the class 6 SSA 405 nm remains near constant at 0.94 and the AAE 405-532 decreases slightly from ca. 7 to 5. Notably, the AAE 405-532 converges towards a common value, around 4, with aging. While there remain some class-specific differences, this indicates that the SOA that is forming has similar optical properties independent of the initial burn conditions. Also, the [OA]/[BC] for class 1 increases by a factor of nearly 70 while the increase for class 6 is 10 times smaller, and the particle class 1 R coat-rBC increases by a factor of 11 while there is negligible change for particle class 6. Generally, the most rapid changes occur when the equivalent aging time is less than a day, with slower changes after this. Some of the observed changes, in particular for class 1 and class 2 particles, result from enhanced loss of BC-rich particles when the lights are turned on, although this alone cannot explain the differing extents of change and would not directly impact the R coat-rBC (Sect. 3.2.1). These observations indicate substantial formation of secondary OA and a net increase in the overall (dilution-corrected) OA, consistent with Lim et al. (2019). If secondary OA formation were offset by evaporation of primary OA then the SSA would not have increased, nor would the [OA]/[rBC] or R coat-rBC ratios have increased.
Additionally, the OA O : C atomic ratio increases and the AMS f 60 (a marker for primary biomass burning OA attributed to levoglucosan and similar species) decreases rapidly with photochemical aging (Fig. 1). However, unlike the above properties, the O : C and f 60 evolution are generally similar between SSA classes, despite some variability in the primary particle properties (McClure et al., 2020). The changes in both O : C and f 60 occur more rapidly than can be explained by heterogeneous oxidation, implying rapid photochemical production of secondary OA .
The O : C increases rapidly at t OH < 1 d with continual in- creases with further aging. The f 60 values decline rapidly at t OH < 1 d to around f 60 = 0.008, changing negligibly with continued aging. It is noteworthy that the f 60 plateaus around 0.008 upon aging rather than at 0.003, the value denoted by Cubison et al. (2011) as the nominal background outside of biomass-burning-influenced areas. This suggests that observations of f 60 values much smaller than 0.008 in am-bient measurements indicate an influence of OA from nonbiomass-combustion sources (both POA + SOA).

Brown carbon Observations
The class-average MAC BrC,405 and the AAE BrC,405-532 evolve with photochemical aging (Fig. 2). Results for individual experiments are shown in Figs. S10 and S11. Overall, the MAC BrC,405 values decrease from the primary values with aging. However, for the initially less absorbing BrC, corresponding to the higher SSA classes (i.e., class 5 and 6), the MAC BrC,405 values first increase at t OH < 1 d before decreasing. This behavior suggests rapid formation of SOA more absorbing than the primary OA for these classes, with production of less-absorbing SOA or conversion of POA or SOA via heterogeneous oxidation into less-absorbing forms at later times (discussed further in Sect. 3.2.2). The MAC BrC,532 values behave similarly (Fig. S12). The classaverage MAC BrC,405 values all converge around 0.2 m 2 g −1 after many days (∼ 5) of equivalent aging. The class-average AAE BrC,405-532 values converge towards AAE BrC,405-532 ∼ 5 after many days of equivalent aging, with the exact behavior dependent on the initial AAE BrC,405-532 .

Comparison with literature
Our observations can be compared with various literature observations, where we use reported SSA or AAE values to infer the equivalent particle class (Table S4). Martinsson et al. (2015) observed that the 370 nm OA absorptivity of class 1 particles decreased after rapidly aging for t OH = 8.3 d. Saleh et al. (2013) reported the AAE for class 1 particles produced from oak combustion changed negligibly (1.38 to 1.42) while the AAE for particles from pine combustion increased slightly (1.48 to 1.73) after photochemically aging smoke for t OH of a few hours; the extent of aging was likely greater for the pine than oak. The AAE for class 1 particles during FIREX increased to a greater extent (1.4 to 2.2) after similar aging (t OH ∼ 6 h). Saleh et al. (2013) also report smaller SOA absorptivity compared to POA at 550 nm, qualitatively consistent with our observations. Zhong and Jang (2014) observed the 550 nm absorptivity of class 5 particles initially increased over ∼ 2 h but then gradually declined upon photochemical aging of smoke from smoldering combustion. This general behavior is consistent with the behavior of the class 5 and 6 particles here, for which the MAC BrC increased slightly in the first few hours of equivalent aging followed by a continuous decline.
Similar to our observations, Kumar et al. (2018) observed AAE 370-660 values for class 1 particles increased from around 1.4 to 2 for photochemically aged beechwood smoke over t OH ∼ 1 d. They report that the primary OA is more absorbing than the SOA formed. We interpolate their results to estimate MAC 405 values for BC (12.4 m 2 g −1 ±1.1), primary BrC (4.0 m 2 g −1 ± 1.3), and secondary BrC (1.6 m 2 g −1 ± 1.4). The MAC BC,405 value agrees well with our estimate of 11.8 m 2 g −1 . However, their primary MAC BrC,405 substantially exceeds our class 1 average (2.25 m 2 g −1 ±1.0) as does their primary BrC AAE (4.6 versus 2.2 ± 1.1, respectively), while their AAE for SOA is similar to that observed here at longer aging times (5.5 versus ∼ 5, respectively). Over their ∼ 1 d of equivalent aging they find little variability in the MAC BrC for SOA. Cappa et al. (2019b) reported MAC BrC,405 and AAE 405-532 for relatively fresh biomass-burning-derived organic aerosol in the ambient atmosphere, reporting values (0.84 m 2 g −1 and 3.02, respectively) similar to those for class 2 particles here. Sumlin et al. (2017) heterogeneously aged class 6 particles with OH and observed negligible changes in the absorptivity and SSA 405 at 1 and 3.5 d of equivalent aging but then a sudden change at 4.5 d of equivalent aging. This differs substantially from our observations, where changes occurred continuously; the reasons for this difference are unclear, although a discontinuous change with increasing exposure is unexpected. Browne et al. (2019) also heterogeneously aged class 6 particles with OH but observed a continuous decrease in the absorptivity with OH oxidation, consistent with the long-term behavior observed here. Wong et al. (2017) photolytically aged (at 300-400 nm) water-soluble and water-insoluble solution extracts of particles from smoldering combustion and observed that the particle absorptivity initially increased over the course of about a day, peaked, and then declined over longer times to below the initial value. While this general behavior is consistent with the evolution of our class 5 and 6 particles, the photon flux here was likely too low for direct photolytic aging to contribute substantially (Z. , especially given the short absolute aging timescale in the mini chamber (tens of minutes). Lee et al. (2014) photolytically aged water-soluble extracts of secondary BrC produced from photooxidation of naphthalene and observed a continuous decrease in the absorptivity, but again with a time constant that was likely too long to have influenced our experiments. Fleming et al. (2020) photolytically aged particles from 12 of the FIREX burns that were collected on Teflon filters. They observed a wide diversity of equivalent lifetimes (referenced to the time-averaged photon flux in Los Angeles, CA) for different BrC chromophores, some of which were quite short (< 1 d). However, the equivalent lifetime of the total absorption was > 10 d for all samples, with a recalcitrant component making up ca. 30 % of the total absorption.
Overall, our results combined with the literature indicate that differences in starting conditions (i.e., particle class) are important to consider when comparing between different photochemical aging experiments on biomass-combustionderived particles. Additionally, it is important consider whether a given experiment is likely to favor one process over another, e.g., SOA formation, heterogeneous oxidation, or photolysis.
3.2 Understanding and modeling the photochemical evolution of smoke 3.2.1 Chamber photochemical model description

Overview
We observe that a wide range of particle properties evolve as the smoke from all SSA classes is photochemically aged.
To facilitate interpretation, we have developed a simplified model of photooxidation that accounts for SOA formation from oxidation of gas-phase species, heterogeneous oxidation, differential losses of particle types, and dilution in the mini chamber. We aim to simulate the evolution of the brown carbon absorptivity (i.e., MAC BrC ), specifically, using the initial primary particle properties, gas-phase species, and evolution of the [OA]/[rBC], O : C, and AMS f 60 as constraints or guides as to the reasonableness of the general model formulation. Model parameters are constrained as possible by the observations or tuned to provide good agreement with the observations for all particle classes (Tables 1 and 2). Our modeling approach complements the analysis of Lim et al. (2019), who show that the amount of SOA formed is directly related to the total amount of pre-cursor nonmethane organic gases (NMOGs) in the chamber and that the effective SOA mass yield increases with aging.
Here, we take a more mechanistic approach to understanding SOA formation in these experiments and focus on the influence of SOA formation on the observed optical properties. The model framework, constraints, and assumptions are described below.

Reactive gases
Biomass burning releases a wide variety of NMOGs and references therein). Upon oxidation, these NMOGs can form SOA. In general, higher-molecular-weight NMOGs have a higher propensity to form SOA (Cappa and Wilson, 2012). We consider the suite of gas-phase compounds measured by PTR-ToF-MS  having molecular weights greater than 50 amu as potential SOA precursor compounds. (Consideration of all species measured, including those with MW < 50 amu does not change the results, consistent with Lim et al., 2019.) These 107 identified gas-phase compounds have been binned according to their OH reaction rate coefficients reported by Koss et al. (2018) (Figs. S13 and S14). The OH rate coefficients range from 3 × 10 −10 cm 3 molecules −1 s −1 (for sesquiterpenes) to 1.4 × 10 −13 (for nitrobenzene); most compounds have k OH values greater than 4 × 10 −12 cm 3 molecules −1 s −1 . Based on these observations, we make a simplifying assumption that there are three general classes of SOA precursor molecules: those that react fast (3 × 10 −10 ≥ k OH > 3 × 10 −11 ), those that react slowly (3 × 10 −11 ≥ k OH ≥ 2 × 10 −12 ), and those that react very slowly (k OH < 2 × 10 −12 ). The corresponding SOA-typespecific k OH values we use in the model are k OH,fast = 4 × 10 −11 cm 3 molecules −1 s −1 (τ OH,fast = 0.19 d), k OH,slow = 9 × 10 −12 cm 3 molecules −1 s −1 (τ OH,slow = 0.86 d), and k OH,VS = 7 × 10 −13 cm 3 molecules −1 s −1 (τ OH,VS = 11 d) (Table 1 and Fig. S13). (The time constants given correspond to [OH] = 1.5 × 10 6 molecules cm −3 .) The dividing lines between the NMOG classes are somewhat arbitrary but capture the general overall behavior and are consistent with variable observed formation timescales of secondary NMOG . Loss of primary species due to photolysis is not considered;  show that rapid photolysis dominates loss for a small number of primary species, notably furfural. These species tend to be fast reacting and thus are incorporated in the fast NMOG group, although their actual loss rate is likely underestimated.
The initial total NMOG concentration is specified relative to the initial [OA], consistent with Lim et al. (2019). The observed average ratio between the total carbon mass concentration measured by the PTR-ToF-MS and the initial [OA] carbon mass is 7 ± 3. SSA-class-specific initial [NMOG]/ [OA] values are specified in the model, con-  strained to fall around this range (Table 2). This initial gas-phase mass is apportioned between the fast, slow, and very slow NMOGs. The PTR-ToF-MS measurements indicate that the relative abundances of fast-reacting, slowreacting, and very slow reacting NMOG average approximately 0.5 : 0.4 : 0.1 on a mass basis. We specify the very slow NMOG fraction as a constant and allow the relative abundances of fast-and slow-reacting NMOGs to vary between the particle classes, with specific values determined from fitting to the observations; the derived values are in general agreement with the observed range (Table 2). Allowing for some variability is reasonable, given that the NMOG composition varied between experiments and with burn type . The influence of multigeneration chemistry is accounted for by assuming all gas-phase products from reaction of primary precursors are reactive towards OH radicals. This multigenerational (MG) chemistry is simplified by assuming that all MG species react identically, independent of the actual generation number (i.e., number of times reacted) or precursor identity. This allows for a substantial reduction in the number of species tracked relative to more explicit meth-ods (Aumont et al., 2005;Cappa and Wilson, 2012). The assumed multigenerational oxidation OH reaction rate coefficient, k OH,MG , is set to 5 × 10 −12 cm −3 molecules −1 s −1 (τ OH,MG = 1.54 d). The k OH,MG falls between the fast and slow species. MG species are assumed to fragment upon reaction, with a fragmentation probability (f ) of 15 %, serving to limit the maximum SOA formation; assuming a constant f is a simplification over more detailed approaches (Cappa and Wilson, 2012).

SOA formation and processing
SOA forms upon reaction of the primary NMOG types and MG species, referred to here as SOA fast , SOA slow , SOA VS , and SOA MG . SOA formation occurs here with fixed yields (α) assuming both instantaneous and irreversible (i.e., nonvolatile) condensation, which are simplifications over more detailed approaches. The influence of vapor wall losses (Zhang et al., 2014) is not explicitly considered and thus reflected in the derived α values. SOA and POA also react heterogeneously with OH, producing oxidized OA that can also react with OH. We assume an OH reactive uptake coefficient (γ OH ) of unity for all OA types. Upon oxidation, 15 % of 8520 C. D. Cappa et al.: Biomass-burning-derived particles from a wide variety of fuels -Part 2 the POA and SOA mass is assumed lost owing to fragmentation and volatilization of the products (i.e., f het,x = 0.15). Heterogeneous oxidation of oxidized OA leads only to fragmentation reflecting the greater propensity for more oxidized species to fragment upon reaction (Kroll et al., 2015). The k OH,het values are calculated using the [OH] with the observed surface-weighted particle diameters and appropriate mass-transfer corrections (Smith et al., 2009).
The overall reaction scheme is summarized below: Reactions (R1)-(R4) represent oxidation of gas-phase species and SOA formation, where SOA i = α i · NMOG i and for a given reaction NMOG MG = (1 − α i )·NMOG i ; the subscript i indicates which NMOG type reacted. Also, SOA het or POA het + OH k OH,het −→ volatile products.
Reaction (R5) represents the heterogeneous oxidation of fast, slow, very slow, or multigeneration SOA and conversion to an oxidized SOA product, while Reaction (R6) represents heterogeneous oxidation of POA to an oxidized product. Reaction (R7) indicates that reaction of oxidized OA only produces volatile products.

Dilution and particle wall losses
Given the semibatch operation method for the mini chamber, the concentration of particles and gases decreased over time owing to dilution and losses to the chamber walls. The non-OH loss rate of gases was assumed constant in the model, consistent with observations during an experiment where the lights were left off. However, we observed that the overall decay of BC particles containing little coating material (e.g., class 1 and class 2) was enhanced when the lights were turned on, while it was not for particles having thicker initial coating amounts (Figs. S15 and S16). This enhanced loss was unique to BB particles, as no such behavior was observed for either atomized fullerene soot (highly absorbing) or ammonium sulfate (nonabsorbing). That enhanced decay occurs for the BC-rich particles suggests that this phenomenon is related to the amount of coating material, since the class 1 and 2 particles have substantially smaller initial R coat,rBC values compared to the other classes ( Fig. 1 and McClure et al., 2020). We speculate that the enhanced loss of BC-rich particles results from their having a greater propensity towards photoelectric charging with the 254 nm light, as photoelectric charging is highly sensitive to the state of the particle surface (Burtscher, 1992). We determined an empirical relationship between the observed time-varying rBC decay rate and the coating amount for use in the model (Fig. S17). The decay rate slows as particles become more coated (i.e., have larger R coat,rBC ), eventually reaching a plateau. We also account for the mixing state of the particles when determining particle loss rates, as McClure et al. (2020) showed that the fraction of total OA that is internally mixed with BC decreases as [OA]/[rBC] increases. We assume that the population of particles containing BC exhibits faster loss than the population that does not. Independent of the enhanced decay for BCrich particles, particle decay is faster than for dilution-driven decay of gases because the particles are more subject to wall losses. The reference decay rates for particles and gases were determined from experiments conducted using atomized ammonium sulfate, atomized fullerene soot, and a "dark" smoke experiment. It is assumed that POA does not evaporate upon dilution in the chamber and thus does not contribute further to the available NMOGs (discussed further in Sect. 3.2.6).

SOA properties and model fitting
The different types of SOA in the model, which form from different NMOGs, can have different properties. The properties that are allowed to differ between SOA types and heterogeneous oxidation products, besides k OH , are the MAC BrC , SOA yields, O : C, and the f 60 (Tables 1 and 2). While allowed to vary between SOA type, these parameters are assumed to be independent of the SSA class. In this manner, we aim to find an overall solution that allows for one set of SOA-type-specific parameters that gives good modelmeasurement agreement for all of the SSA classes. Our analysis focuses on the evolution of the particle optical properties and specifically the BrC absorptivity. Sect. 3.2.2 provides a detailed discussion of the evolution of the MAC BrC with oxidation and the associated determination of SOA-type-specific MAC BrC values. Values for the other parameters (SOA yields, O : C and the f 60 ) are briefly discussed here. The tuned SOA yields were α fast = 0.43, α slow = 0.15, α VS = 0.05, and α MG = 0.45. These are effective yields averaged across all NMOGs of a given type. The derived average SOA yields are within the range of SOA yields expected for the individual precursor species (Bruns et al., 2016).
Tuned values for the O : C for the SOA types are consistent with expected physical behavior, guided by singlecomponent studies (Chhabra et al., 2011). The fit O : C atomic ratios of the first-generation SOA formed are 0.73 (fast), 0.59 (slow), and 0.59 (very slow, assumed to be the same as slow). The O : C of multigeneration SOA and heterogeneously oxidized POA and SOA vary with time, with the model fit indicating 1.22 oxygen atoms added per oxidation reaction, generally consistent with expectations (Kroll et al., 2015). The model agrees well with the observations (i) when the f 60 values for the various SOA types are f 60,fast = 0.008, f 60,slow = f 60,VS = 0.003, and f 60,MG = 0.006 and (ii) when the f 60 for the heterogeneous oxidation products are assumed to depend on the identity of the oxidized component, with f 60,het = 0.01 for SOA oxidation, f 60,het = 0.003 for externally mixed POA oxidation, and f 60,het = 0.008 for internally mixed POA oxidation. We note that similar results are is the high-resolution ion at m/z = 60 that most corresponds to levoglucosan.)

Model-measurement comparison
The optimized model does a good job (reduced chi-square = 0.4) of describing the evolution of MAC BrC , [OA]/[rBC], O : C atomic ratio, and AMS f 60 (Fig. 3). The reasonable agreement for [OA]/[rBC] indicates the appropriateness of the empirical correction for enhanced decay of rBCcontaining particles, the specified SOA yields and initial [NMOG]/[OA] ratio, and the apportionment between the different NMOG types. The model-measurement agreement improves if the unknown model parameters are allowed to vary somewhat between particle classes; again, some variability is expected given the burn-to-burn variability in the mix of NMOG species . However, that use of class-independent parameters provides for a generally good description across classes demonstrates an overall general nature of the photochemical evolution.
The evolution of the MAC BrC , [OA]/[rBC], O : C atomic ratio, and AMS f 60 derives from changes in the OA composition. Examples of the simulated time-dependent variation in OA composition for particle class 1 and class 6 are shown in Fig. 4. The observations demonstrate the importance of SOA formation, with the predicted fractional contribution of POA decreasing over time. For class 1, the MAC BrC decays rapidly owing to a large fraction of the POA being internally mixed The SOA fast is substantially more absorbing than the other SOA types. It is difficult to estimate a comprehensive uncertainty on these values; the above uncertainties were qualitatively estimated based on the model sensitivity to changing the parameter values (see Supplement). The strong absorptivity of the fast-forming SOA and the substantial difference between MAC fast and MAC slow and MAC 2G are unexpected and somewhat surprising. The identities of the likely precursor NMOG characterized  can be interrogated to understand this difference along with the evolving chemical conditions in the chamber.
SOA absorptivity varies between precursors (Lambe et al., 2013;Romonosky et al., 2016;Xie et al., 2017), suggesting different precursors contribute differentially to the SOA absorption here. Monoterpenes form SOA that is non-toweakly absorbing. In contrast, SOA from aromatic precursors can be quite absorbing, more so in the presence of NO x . Formation of nitroaromatics is often linked to the enhanced absorptivity when NO x is present, and condensed-phase reactions producing highly conjugated, potentially N containing compounds also contribute to light absorption . Garmash et al. (2020) recently reported ROOR dimer formation in the gas phase from OH oxidation of aromatics, which we speculate could also contribute to light absorption.
Given the potential importance of nitroaromatic formation to SOA light absorption, the organonitrogen (ON) aerosol contribution here is characterized from the HR-AMS using the method of Kiendler-Scharr et al. (2016;see Supplement in McClure et al., 2020). (We use the term "organonitrogen" quite generally here, as the measurements do not directly provide the particular chemical nature of the N-containing organic species, which could be nitroaromatics or organic nitrates. Further work is required to quantitatively differentiate ON functionalities in the AMS. The slow and very slow NMOG and the MG species are, apparently, comparably less likely to form ON in our experiments, leading to a decline in their relative contribution to OA. That the observed [ON]/[OA] ratio first increases then decreases with aging while the average MAC BrC derived for the SOA decreases with aging (owing to the MAC fast > MAC 2G > MAC slow = MAC VS ) suggests a relationship between the processes driving these behaviors as well as a shift with aging. While the [ON]/[OA] ratio would depend on the formation of any organonitrogen species, the SOA absorption likely depends, at least in part, on nitroaromatic formation. Organic nitrates form from reaction of NO with peroxy radicals (RO 2 ), which competes with RO 2 + HO 2 , RO 2 + RO 2 , and RO 2 autoxidation and is thus sensitive to variations in the availability of NO (Orlando and Tyndall, 2012;Bianchi et al., 2019). However, nitroaromatics typically form in the gas phase from reaction of NO 2 with phenoxy radicals or with OH-aromatic adducts (Grosjean, 1984;Berndt and Böge, 2003;Vereecken, 2019). Phenoxy radicals generally derive from OH reaction with phenolic molecules and both NO and O 3 compete with NO 2 for reaction with phenoxy radicals; products from reaction with NO and O 3 are not well established (Vereecken, 2019). The importance of the OH-aromatic adduct +NO 2 pathway to nitroaromatic formation is suggested as small for species such as toluene and phenol owing to efficient reaction with O 2 (Atkinson et al., 1992;Vereecken, 2019), although it has been proposed as the major pathway for nitroaromatic formation from guaiacol and similar species (Lauraguais et al., 2014;Sun et al., 2019).
The [NO]/[NO 2 ] ratio in the primary smoke varied from 4.88 to 0.84 . Modeling by  for a few of the experiments indicates a rapid decrease in the [NO]/[NO 2 ] ratio towards zero with time owing to inefficient photolysis of NO 2 in the mini chamber. Consequently, organic nitrate formation should be fastest early on, becoming very small as time progresses. This can help explain the observed dependence of [ON]/[OA] on aging. However, as nitroaromatic formation involves NO 2 , rather than NO, the evolving [NO]/[NO 2 ] would not explain the evolution of the MAC BrC . The fast-reacting aromatics (e.g., guaiacol, syringol, eugenol, styrene, vanillin, vinyl guaiacol, creosol, catechol) tend to be more substituted than the slow-reacting aromatics (e.g., phenol, o-cresol, toluene, benzaldehyde, tolualdehyde, naphthalene). SOA formed from guaiacol with NO x present is substantially more absorbing than SOA from either toluene or m-xylene (Romonosky et al., 2016). Additionally, the nitroaromatic yield from reaction of guaiacol exceeds that of phenol, reflecting, in part, faster H abstraction from the phenol group in more substituted aromatics (Harrison et al., 2005;Lauraguais et al., 2014), and production of nitroaromatic species from reaction of nonphenolic molecules, such as toluene, requires multiple reactions with OH. Thus, it may be that the fast-reacting aromatic species generally produce more-absorbing nitroaromatic species with higher SOA yields compared to the slowreacting aromatic species, contributing to the decrease in both the [ON]/[OA] and the MAC BrC with aging in the mini chamber.
Analogous to the treatment of the MAC BrC for SOA, we have attempted to model the ON formation by assigning a NMOG-type-specific, yet particle-class-independent, ON yield. Unlike the MAC BrC , no model parameters allow for good model-measurement agreement using this approach. This primarily results from the different particle classes having very different [ON]/[OA]. For example, for the [ON]/[OA] ratio for class 1 particles to increase from the initial value (5.7 %) to the peak value (18 %) requires a much larger model ON species SOA yield than for the class 6 particles, for which the [ON]/[OA] increases from 0.3 % to only 0.6 %. The reason for these substantial differences likely relates to the factors discussed above.
The reasonableness of the derived MAC BrC values for SOA is assessed by estimating approximate upper (high NO x ) and lower (low NO x ) MAC BrC values for the SOA types based on literature MAC values for SOA from individual precursors (Romonosky et al., 2016), the NMOG emission factors , and estimated SOA yields (Bruns et al., 2016): where x is the SOA type and i is for an individual NMOG. We note the highly uncertain nature of these estimates and therefore only consider them qualitatively. The estimated MAC BrC,fast values fall in the range 0.3 m 2 g −1 (low NO x ) to 2.4 m 2 g −1 (high NO x ). This encompasses contributions from highly absorbing and abundant guaiacol SOA, moderately absorbing benzene diol (and related species), and effectively nonabsorbing monoterpene SOA. For slow SOA, the estimated MAC BrC,slow ranges from 0.1 to 0.6 m 2 g −1 , encompassing major contributions from moderately absorbing phenol and cresol SOA. The estimated MAC BrC,VS de-8524 C. D. Cappa et al.: Biomass-burning-derived particles from a wide variety of fuels -Part 2 pends almost entirely on the benzene SOA, ranging from 0.21 m 2 g −1 (low NO x ) to 0.88 m 2 g −1 (high NO x ). Our derived MAC BrC,fast falls between the upper and lower estimates, while the MAC BrC,slow , MAC BrC,VS , and MAC BrC,MG are more similar to the lower estimates.

Extending the mini chamber results to the atmosphere
In the experiments, particles and gases experience different decay rates, with particle loss rates exceeding NMOG precursor loss rates and the loss rates of BC-rich particles enhanced. The model allows for simulation of the evolution of the overall system in the absence of such experimental differences by setting the dilution of all components to the same value and wall losses to zero. This provides insights into the likely influence of photochemical oxidation on the evolution of smoke in the atmosphere, although it likely does not fully account for the influence of NO x and the evolving NO/NO 2 ratio. For simplicity, we use a dilution rate of zero for these atmospheric simulations, but any value could be used so long as the focus is on variability in intensive properties. Simulated OA composition profiles are compared for particle classes 1 and 6, as examples, for chamber ("chm") and atmospheric ("atm") simulations in Fig. 4. In the atmospheric simulations, the POA influence persists to much longer times than in the chamber simulations. For example, for class 1 the POA fraction after 2 d of equivalent aging is 0.05 for the chamber simulation but 0.35 for the atmospheric simulations; for class 6 the increase in the POA fraction, from 0.2 (chamber) to 0.3 (atmospheric), is smaller but still notable. Some of the increase in the POA contribution for the atmospheric versus chamber simulations results from the POA and NMOG having the same loss rates in the atmospheric simulations. This leads to a decreased relative contribution of SOA. The larger difference between the atmospheric and chamber simulations for particle class 1 also reflects the comparably greater influence of enhanced decay of BC-rich particles.
The fractional contribution of the second-generation SOA decreases in the atmospheric simulations for all classes. This too results from the particle decay rate equaling the gas decay rate in the atmospheric simulations. In the chamber simulations, the OA is lost at a faster rate than the gases, and thus the second-generation SOA, which forms later than the fast and slow SOA, is effectively enhanced; this enhancement does not influence the atmospheric simulations. There is little difference in the fractional contribution of heterogeneous oxidation products between simulations, a consequence of the ensemble treatment of heterogeneous oxidation products here.
Differences between the chamber and atmospheric simulations are shown in Fig. 6  ratio. Averages across all particle classes are shown to facilitate compari-son; atmospheric simulation results for individual particle classes are compared with the observations in Fig. S20. Given the relatively large (albeit particle class dependent) absorptivity of the POA, the MAC BrC,atm decays more slowly than the MAC BrC,chm . This is accentuated by the fraction of fast SOA being somewhat greater at longer aging times for the atmospheric simulations, since the MAC fast > MAC sec > MAC slow . The evolution of the MAC BrC for the atmospheric simulations is empirically well described by a biexponential decay. A fit to the model prediction for the average behavior across all classes (Fig. 6)

Secondary OA versus heterogeneous oxidation
The particle properties evolve from both SOA formation and heterogeneous oxidation. To separate these processes, two additional sets of model simulations are run: (i) with the gas-phase rate coefficients set to zero such that only heterogeneous oxidation occurs, and (ii) with the OH uptake coefficient set to zero, and thus only SOA formation occurs (Fig. 6). It is evident that the evolution of all intensive properties occurs much more slowly with only heterogeneous oxidation. With heterogeneous oxidation only, the class-average MAC BrC,405 decays to a much lesser extent, even for the atmospheric simulations. Similarly, the increase in O : C is much too small and the AMS f 60 decays to a much lesser extent. The OA-to-BC ratio for the heterogeneousonly simulations differs notably from the full simulations. For the heterogeneous-only chamber simulations, this ratio increases initially until about 1.5 d of aging, at which point it decreases. The decrease results from loss of mass over time from fragmentation, while the increase results from faster loss of BC-rich particles in the chamber. For the atmospheric simulations, the OA-to-BC ratio decreases continuously when only heterogeneous oxidation is included. In contrast, for most properties the SOA-only simulations differ by only small amounts from the full simulations. The exception is the MAC BrC , for which the decrease in the class-average value with time is notably smaller in the SOA-only simulation compared to the full simulation for both chamber and atmospheric simulations. Our simulations assumed an OH reactive uptake coefficient of unity. We note that if a substantially larger value is assumed (γ OH ∼ 10), the predicted changes due to heterogeneous oxidation are much larger and reasonably in line with the observations. Values substantially greater than unity have been found for some chemical systems (Richards-Henderson et al., 2016;Schnitzler and Abbatt, 2018), but for compounds such as levoglucosan -a notable component of BB particles -values less than unity are common (Kroll et al., 2015).
Under the assumption that γ OH ≤ 1 for BB particles, these observations point to an important conclusion that is in line with various ambient observations. Large changes in key intensive properties of BB particles, such as O : C and AMS f 60 , result primarily from secondary OA formation, with heterogeneous oxidation having a smaller influence. While the BrC absorptivity is comparably more sensitive to heterogeneous oxidation, SOA formation remains the major driver of the observed changes. Thus, in ambient observations of biomass burning plumes (Vakkari et al., 2014;Forrister et al., 2015;Garofalo et al., 2019), a notable increase in the O : C (or related measures) and a decrease in the f 60 can be taken as a clear indication of SOA formation.

Absolute absorption
The observations indicate that the observable (i.e., bulk average) MAC BrC decreases with photochemical aging. However, this results primarily from mixing of absorbing POA with various types of absorbing SOA, with some contribution from heterogeneous oxidation. As such, the absolute absorption in the atmospheric simulations typically increases over time, at least initially, due to the production of new, absorbing particle mass. The exact behavior is particle-classspecific (Fig. 7). The initial increase slows over time as the pool of NMOG precursors depletes. At even longer times the absolute absorption for some classes decreases as heterogeneous oxidation converts more-absorbing BrC (specifically, POA and SOA fast ) into less-absorbing BrC and engenders some mass loss over time due to fragmentation. However, this is only true for some of the particle classes. The simulations indicate that, on average, after 1 d of equivalent aging the absolute absorption increases by a factor of 1.6 owing to production of new, absorbing OA mass.

POA volatility and the impact of dilution
Upon dilution, semivolatile particle components may evaporate, which should lead to a decrease in the OA-to-BC ratio and, potentially, changes in other particle properties; the MAC BrC could change if the absorptivity of the evaporating versus low-volatility (or nonvolatile) components differs. Given the semibatch operation (Sect. 2.2), substantial, continual dilution occurs throughout an experiment. Rapid dilution also occurs upon sampling of smoke into the clean mini chamber air. Dilution-driven evaporation has been suggested as an important factor in the chemical evolution of BB in ambient biomass burning plumes (Hodshire et al., 2019).  We assessed the impact of continual dilution on our observations by conducting one experiment during which the chamber was left dark, although ozone was present at about 50 ppb (Fig. 8). The primary particles corresponded to class 3 particles (SSA 405 nm = 0.73). After sampling, the OA and rBC concentrations decreased by about a factor of 33 over 45 min owing to dilution and other losses. For comparison, the [ACN] dilution tracer decreased by a factor of 21.
During this experiment the [OA]/[rBC] ratio was nearly constant (19.6 ± 0.7, 1σ ), even slightly increasing over time. Also, the O : C remained constant (0.39±0.03, 1σ ), as did the H : C (1.74 ± 0.01, 1σ ). These observations together indicate that there was little, if any, evaporative loss of OA. However, the AMS f 60 declined continually, by about 30 %. The signal at m/z = 60 is only a small fraction of the total OA, and thus changes in f 60 can occur even if only small changes in total mass occur. The AMS f 60 could also evolve over time from in-particle reactions that occur even in the absence of oxidants. The mass fraction of OA remaining (MFR OA ) after heating in the thermodenuder increased slightly over time, from 0.05 to 0.07. This could indicate evaporation of more volatile components, although it could result from "ripening" of the particles over time (Tritscher et al., 2011).
SOA from reaction of some NMOGs with O 3 may have offset some evaporative OA mass loss, keeping the total OA mass constant while the f 60 and MFR org changed. Monoterpenes are the most important SOA precursor class here that reacts readily with O 3 . The measured initial monoterpene concentration (8.6 ppb = 50 µg m −3 ) constrains the potential SOA formed. Accounting for differential losses of particles and gases in the mini chamber, with 50 ppb O 3 and an assumed SOA yield of 0. The reason for the insensitivity to dilution of our experiments may result from the concentration range considered. May et al. (2013) established the volatility distribution for biomass burning OA from thermodenuder measurements. They compared predictions from their derived volatility distribution to observations of OA emission factors for different fuel types at varying levels of dilution and initial concentrations. At the lowest initial [OA] (∼ 100 µg m −3 ), active dilution had little influence and in some cases the OA emission factor actually increased after dilution in their experiments. In contrast, when the initial [OA] was much larger, on the order of 1000 µg m −3 , there was a clearer relationship between the OA emission factor and the OA concentration and better agreement with their predictions. For comparison, in our experiments, the initial [OA] in the mini chamber had a geometric average of 76 µg m −3 , ranging from 8 to 384 µg m −3 ; notably, the dark experiment was at the highest initial [OA]. Dilution into the mini chamber was a factor of 7. Most likely, evaporation resulting from dilution occurred upon initial injection of the particles into the mini chamber with little additional evaporation as experiments progressed, to the extent that the particles evaporated much at all.

Comparison with ambient observations
There are very few ambient assessments of how photochemical oxidation influences brown carbon absorptivity. Forrister et al. (2015) measured dilution-corrected water-soluble plus methanol-soluble BrC absorption in aboveground ambient wildfire plumes at various distances downwind from the fires. The measured O : C and AMS f 60 changed with time as the BrC absorption decreased, indicating that chemical changes occurred as the plume aged. They observed that the absolute BrC absorption decreased over time, with a timescale of only 10 h; this was associated with a decay in the AAE determined from in situ measurements. Surface measurements of aged smoke plumes by Selimovic et al. (2019) are also suggestive of a decay in the AAE with aging. The BrC decay time from Forrister et al. (2015) is substantially faster than we observe for any of the particle classes. Interestingly, we predict that over 10 h the absorption by BrC in a wildfire plume should have increased, and only at much later times should it have decreased (Fig. 7). In the case where only heterogeneous oxidation is included (with γ OH = 1), the predicted decay in BrC absorption based on our observations has a timescale of ca. 4 d, substantially slower than observed by Forrister et al. (2015).
It is possible that the smoke sampled by Forrister et al. (2015) differed significantly from any of the burns sampled here. However, this seems unlikely given the wide range of fuels and burn conditions considered here and since the plumes sampled by Forrister et al. (2015) likely derived from combustion of similar fuels as used here. Also unlikely is that greater dilution in the atmosphere played an important role, as it is thought that more-absorbing primary OA has lower volatility than less-absorbing primary OA (Saleh et al., 2014). Thus, it is possible that the difference between Forrister et al. (2015) and our results indicates that direct photobleaching rapidly degrades BrC absorptivity, as direct photolysis in our experiments was likely of minimal importance owing to the relatively low light intensity, single initiation wavelength (254 nm), and short absolute timescale (< 1 h) compared to the atmosphere.
However, an additional difference is that we measured absorption by suspended particles at low-to-moderate relative humidity, whereas Forrister et al. (2015) characterized BrC absorption after extracting material collected onto filters into water and then methanol. It is possible that solvent extraction alters the BrC absorptivity in some OA-compositiondependent manner, leading to an apparent time-dependent decay in the BrC absorption. Consistent with this suggestion, Fleming et al. (2020) reported that (i) the total absorptivity lifetime of BB particles photolytically aged on a filter greatly exceeded that of individual chromophores (> 10 d versus < 2 d) and (ii) the apparent changes in total absorption depended on whether the absorption was measured for particles on the filter versus for solution extracts. There is also evidence that the larger molecules comprising OA from biomass burning, which are often more absorbing yet less soluble than small molecules (Di Lorenzo et al., 2017;Saleh et al., 2018), are less susceptible to photobleaching (Wong et al., 2017(Wong et al., , 2019. This could lead to absorption measurements from solvent extracts overestimating the effects of photo-bleaching. Nonetheless, the suggestion that the measurement method contributes to the lab-field difference remains speculative as direct, quantitative comparisons between BrC absorption measured for suspended particles versus from solution extracts are limited; we suggest that targeted comparisons between absorption measurement methods would be informative. Wang et al. (2016) also characterized changes in BrC absorptivity of BB particles in the Amazon. They found that the BrC absorptivity decreased initially over an estimated ca. 20 h of photochemical aging, after which the absorptivity remained constant. As above, this timescale seems too short for heterogeneous oxidation to have a major impact, thus implicating direct photolysis as the reason for the photobleaching. However, there are two important considerations. First, Wang et al. (2016) note that they cannot rule out production of less-absorbing SOA as the reason for the absorptivity decrease. While the OA concentration was constant over time and therefore suggestive of little SOA formation, it may be that dilution of the plume offset SOA formation and consequently that SOA formation precipitated the decrease in absorptivity. Second, their estimated lifetimes are determined from NO x losses and thus sensitive to assumptions about the average OH; as such, longer lifetimes cannot be ruled out.
Finally, Zhang et al. (2017) characterized water-plusmethanol-extracted BrC in the outflow of storm clouds and, in one case, were able to measure BrC absorption for freshly expelled particles versus particles sampled 1 d later. The BrC absorptions for the fresh and aged particles were nearly identical, with no indication of bleaching despite the high altitude, 11 km, and thus high UV photon flux. Thus, this study indicates that photobleaching of BrC may have little influence on at least some types of BrC. Further, Zhang et al. (2017) report absolute absorption values that, it seems, are not dilution corrected. Thus, the constancy of the absolute absorption between the fresh and aged particles implies potential BrC production, as dilution is expected. Ultimately, further experiments investigating direct photolysis of biomass-derived BrC and additional field observations of the evolution of BrC absorptivity will be necessary to reconcile our findings and the limited number of field observations.

Conclusions
We characterized the photochemical evolution of smoke (particles + gases) produced from combustion of a wide variety of biomass fuels. Particle properties were characterized as a function of equivalent photochemical aging, with a focus on the particle optical properties. Photochemical aging led to dramatic changes in the particle chemical composition, as evidenced by a large and rapid increase in the O : C atomic ratio of the organic aerosol and a decrease in the marker ion f 60 in the OA mass spectrum. These chemical changes occurred concurrent with large changes in the [OA]/[rBC] ra-tio, indicating substantial production of secondary organic aerosol mass. The particle optical properties also changed substantially upon aging. Experiments were classified into six classes according to the SSA of the primary particles. The average evolution of the optical properties of particles in each class was characterized; the observed behavior was generally class specific. The total particle absorptivity normalized to black carbon (the MAC BC ) generally increased with aging due to production of new, somewhat absorbing OA. The single-scatter albedo also generally increased with aging, although to a much lesser extent for experiments in which the initial particles already had a large SSA. The absorptivity of the organic aerosol components, i.e., of the brown carbon mass absorption coefficient (MAC BrC ), exhibited class-specific behavior. For particles having an initially large SSA, the MAC BrC exhibited an initial increase at short times (< 0.5 d of equivalent aging) but then decreased monotonically with continued aging. For particles having an initially small SSA, there was a rapid decline in the MAC BrC at short times and then a continued slower decline at longer times. At long times the MAC BrC for the high-SSA and low-SSA initial particles behaved similarly.
The evolution of the BrC absorptivity was shown via application of a mechanistic model to be consistent with a combination of production of strongly absorbing and much more weakly absorbing secondary OA, along with heterogeneous conversion of absorbing POA and SOA into a less-absorbing oxidized OA. This was the case for all particle classes. The SOA formed could be distinguished into four general types: (i) a fast-forming, relatively highly absorbing type; (ii) a more slowly forming, weakly absorbing type; (iii) a very slowly forming, weakly absorbing type; and (iv) a weakly absorbing, second-generation type. The relative abundances of these different types were similar between the different particle classes. The combination of SOA formation and heterogeneous oxidation causes the MAC BrC to evolve in time on three timescales: (i) an initial rapid increase, occurring at aging times < 0.25 d; (ii) a moderately fast decrease, occurring with a timescale of ∼ 1 d; and (iii) a longer decay, occurring with a timescale of about ∼ 1 week. Our results demonstrate that, while primary particle properties derived from biomass combustion can vary dramatically in terms of their properties, the overall evolution upon photochemical aging is reasonably independent of the initial conditions. Data availability. All data used to create this paper are available at https://www.esrl.noaa.gov/csl/projects/firex/firelab/ (National Oceanic and Atmospheric Administration, 2020) and in Cappa et al. (2019a).
Author contributions. CDC and JHK designed the experiments. CDC, CYL, DHH, MC, AK, TBO, and KS carried out the measurements and data processing, with additional assistance from CW and JdG. CDC and CL analyzed data. CDC wrote the manuscript, with contributions from all coauthors.
Competing interests. The authors declare that they have no conflict of interest.