Measurement report: Variability in the composition of biogenic volatile organic compounds in a Southeastern US forest and their role in atmospheric reactivity
- 1Department of Civil and Environmental Engineering, Virginia Tech, Blacksburg, VA 24061, USA
- 2Department of Environmental Sciences, University of Virginia, Charlottesville, VA 22904, USA
- 3Department of Biology, University of Virginia, Charlottesville, VA 22904, USA
Correspondence: Deborah F. McGlynn (email@example.com) and Gabriel Isaacman-VanWertz (firstname.lastname@example.org)
Despite the significant contribution of biogenic volatile organic compounds (BVOCs) to organic aerosol formation and ozone production and loss, there are few long-term, year-round, ongoing measurements of their volume mixing ratios and quantification of their impacts on atmospheric reactivity. To address this gap, we present 1 year of hourly measurements of chemically resolved BVOCs between 15 September 2019 and 15 September 2020, collected at a research tower in Central Virginia in a mixed forest representative of ecosystems in the Southeastern US. Mixing ratios of isoprene, isoprene oxidation products, monoterpenes, and sesquiterpenes are described and examined for their impact on the hydroxy radical (OH), ozone, and nitrate reactivity. Mixing ratios of isoprene range from negligible in the winter to typical summertime 24 h averages of 4–6 ppb, while monoterpenes have more stable mixing ratios in the range of tenths of a part per billion up to ∼2 ppb year-round. Sesquiterpenes are typically observed at mixing ratios of <10 ppt, but this represents a lower bound in their abundance. In the growing season, isoprene dominates OH reactivity but is less important for ozone and nitrate reactivity. Monoterpenes are the most important BVOCs for ozone and nitrate reactivity throughout the year and for OH reactivity outside of the growing season. To better understand the impact of this compound class on OH, ozone, and nitrate reactivity, the role of individual monoterpenes is examined. Despite the dominant contribution of α-pinene to total monoterpene mass, the average reaction rate of the monoterpene mixture with atmospheric oxidants is between 25 % and 30 % faster than α-pinene due to the contribution of more reactive but less abundant compounds. A majority of reactivity comes from α-pinene and limonene (the most significant low-mixing-ratio, high-reactivity isomer), highlighting the importance of both mixing ratio and structure in assessing atmospheric impacts of emissions.
Biogenic volatile organic compounds (BVOCs) are a dominant source of reactive carbon in the atmosphere, with an estimated 90 % of BVOCs emitted from natural ecosystems (Guenther et al., 1995, 2012). In the presence of nitrogen oxides (NOx≡ NO + NO2), BVOCs can react to form tropospheric ozone (O3), which has deleterious effects on human health and ecosystems (Lim et al., 2012; Avnery et al., 2011a, b; Kroll and Seinfeld, 2008). These reactions also result in the formation of lower volatility gases and secondary organic aerosol (SOA) (Atkinson and Arey, 2003; Guenther et al., 1995; Kroll and Seinfeld, 2008; Hallquist et al., 1997), which have direct and indirect effects on the radiative balance of the atmosphere (Intergovernmental Panel on Climate Change, 2013). Once emitted, BVOCs react with and destroy O3 or produce O3 through reactions with other oxidants (in particular, the hydroxyl radical) (Wolfe et al., 2011; Kurpius and Goldstein, 2003). The impact of plant emissions on net O3 production versus loss depends on mixing ratios of NOx, as well as the specific chemistry of the BVOCs emitted (Trainer et al., 1993; Peake and Sandhu, 1983; Pusede et al., 2014). Changes in environmental conditions, pollution levels, phenology, and ecological succession affect plants and ecosystems in ways that change their BVOC emissions and ozone uptake (Sadiq et al., 2017; Zheng et al., 2017; Faiola et al., 2019; Lerdau et al., 1997).
BVOC emissions consist largely of terpenes, including isoprene (C5H8), monoterpenes (C10H16), sesquiterpenes (C15H24), and diterpenes (C20H32) (Kesselmeier and Staudt, 1999; Laothawornkitkul et al., 2009; Guenther et al., 2012). These compounds vary widely in their reaction rates with atmospheric oxidants, so the impacts of BVOC emissions on regional atmospheric chemistry and composition vary with atmospheric composition and species composition of the dominant vegetation (Geron et al., 2000; Claeys et al., 2004; Lee et al., 2006; Goldstein and Galbally, 2007; Hoffmann et al., 1997; Atkinson et al., 1992). Compounds that are acyclic or cyclic with endocyclic double bonds tend to react faster with oxidants due to the higher substitution of the alkenyl carbons in contrast to exocyclic double bonds, which often have one unsubstituted alkenyl carbon (Hatakeyama et al., 1989). Endocyclic monoterpenes (e.g., myrcene, limonene, and Δ3-carene) and sesquiterpenes (e.g., α-humulene and β-caryophyllene) (Atkinson and Arey, 2003; Matsumoto, 2014) also have a greater aerosol formation potential because C–C scission of the double bond is less likely to produce high-volatility fragments (Friedman and Farmer, 2018). Additionally, previous studies that have assessed the reactivity of OH and O3 have found that higher molecular-weight BVOCs are emitted at lower rates but that they make up an outsize percentage of OH and O3 reactive loss due to their faster reaction rates (Yee et al., 2018; Holzke et al., 2006; Helmig et al., 2006). Therefore, detailed speciated BVOC data are important for understanding the reactivity and formation of ozone and SOA. Furthermore, long-term and detailed measurements of BVOCs can assist in reducing inaccuracies in modeled BVOC emissions and in understanding their contribution in ozone and SOA formation (Porter et al., 2017).
The chemical complexity of BVOCs presents a challenge in understanding both atmospheric oxidant interactions and SOA production and composition. This problem becomes more complex in a changing climate and, subsequently, with changing ecosystems. For example, emissions have been found to increase during a forest thinning event (Goldstein et al., 2004) and decrease during times of severe drought and elevated CO2 (Holopainen et al., 2018; Demetillo et al., 2019). Additionally, increased herbivory has been shown to increase both total plant emissions and the relative proportion of sesquiterpenes, which in turn affects SOA production and composition (Faiola et al., 2018, 2019). Therefore, understanding oxidant budgets, SOA formation, and future changes to ecosystems and atmospheric composition requires a detailed chemical understanding of BVOCs.
BVOCs have been the subject of a large number of measurements and studies, and an exhaustive overview of available datasets is outside of the scope of this paper. Generally, measurement campaigns make trade-offs between temporal resolution, chemical resolution, and long-term instrument stability. Many campaigns of a few weeks to a few months have provided chemically detailed (i.e., isomer-resolved) measurements of BVOCs with time resolution on the order of hours (Park et al., 2010; Goldstein et al., 2004; Schade and Goldstein, 2003; Schade et al., 1999; Gilman et al., 2009), while longer term (multi-season or multi-year) measurements tend to achieve lower temporal resolution (Holdren et al., 1979; Guenther et al., 1996; Simpson et al., 2012). Some measurements have provided temporal resolution on the order of minutes using direct mass spectrometry (e.g., proton transfer reaction mass spectrometry (Fares et al., 2010; Kalogridis et al., 2014; Ghirardo et al., 2010; Davison et al., 2009; Greenberg et al., 2003), but these instruments are unable to resolve isomers that may differ substantially in their reactivity and physicochemical properties. A few measurement campaigns have collected long-term (many months), temporally resolved (hourly), and chemically detailed (isomer-resolved) measurements of a range of BVOCs (Read et al., 2009; Kramer et al., 2015; Panopoulou et al., 2020; Millet et al., 2005; Schade and Goldstein, 2001; Plass-Dülmer et al., 2002; Maria Yanez-Serrano et al., 2018; Hellén et al., 2018), but the number of such campaigns is fairly limited, and very few are currently ongoing. These long-term, temporally and chemically detailed measurements are important for understanding the impacts and behavior of BVOCs on timescales relevant to atmospheric processes, from intra-daily to inter-annually. Therefore, to further advance understanding of the role of biogenic emissions in reactions of atmospheric oxidants on the timescale of hours to seasons, we present 1 year of temporally and chemically resolved BVOC measurements in a forest canopy that is representative of many ecosystems in the Eastern and Southeastern US, as part of an ongoing measurement site, with measurements planned to continue for the indefinite future. We examine here the temporal and seasonal patterns of BVOCs that drive oxidant reactivity. The specific focus of this work is to understand the extent to which composition of major BVOC classes may vary and how minor but reactive components may drive oxidant chemistry. A major outcome of this work is a detailed characterization of monoterpenes that may allow model descriptions and non-isomer-resolved measurements of this chemical class to more accurately capture its impacts on tropospheric chemistry.
2.1 Instrument location and operation
In-canopy BVOC volume mixing ratios were measured at the Virginia Forest Research Facility (37.9229∘ N, 78.2739∘ W), located in Fluvanna County, Virginia (McGlynn and Isaacman-VanWertz, 2021). The site is located on the east side of the Blue Ridge Mountains and receives some anthropogenic influence from Charlottesville, VA, and surrounding counties, located 25 km to the west of the site. Ambient temperature in the winter and spring months of January–April (due to data availability) was 9.6 ± 9.4 ∘C and in the summer and fall months (May–October) was 24.3 ± 7.1 ∘C (Fig. S1 in the Supplement). Downwelling shortwave radiation was lower in the winter and spring months (141.4±214.8 W m−2) than the summer and fall months (January–April) on average (235.6±455.4 W m−2) and exhibited lower variability (Fig. S1). The forest canopy consists predominantly of maple, oak, and pine and is approximately 24 m tall (Chan, 2011). Roughly three-quarters of trees in the forest are species that shed their leaves in the fall and winter months. Tree species found at the site range from being predominantly isoprene emitters, such as oak, to predominantly monoterpene and sesquiterpene emitters, such as conifers (Fuentes et al., 1999). Further information pertaining to tree species at the site can be found in Chan (2011). The site houses a 40 m meteorological tower, with a climate-controlled, internet-connected lab at the bottom that is supplied by line power, known alternately as “Virginia Forest Research Lab” (VFRL) and “Pace Tower”. The measurement period included in this work extends from 15 September 2019 to 15 September 2020, though measurements are ongoing and are anticipated to continue for several years. All results describing seasonality are divided into two separate seasons based on approximate frost dates: the growing season (May–October) and non-growing season (November–April).
Figure 1 depicts the sampling and instrumentation configuration for the automated gas chromatograph–flame ionization (GC-FID) detector used to quantify BVOC volume mixing ratios (the VOC-GC-FID). Air is pulled from mid-canopy (∼20 m above ground level) at 1400 sccm through a 1/8 in. i.d. Teflon tube in an insulated waterproof sheath held at 45 ∘C. The residence time of an air sample in the inlet is about 8 s. Ozone is removed from the sample using a sodium-thiosulfate-infused quartz fiber filter (Pollmann et al., 2005) at the front of the inlet. Efficacy of the ozone scrubber was empirically tested by measuring removal over a multi-week exposure to ozone concentrations several times higher than ambient levels. Efficacy was confirmed following deployment by verifying ozone removal of removed filters. A subsample of ∼70 sccm is concentrated onto a multibed adsorbent trap composed of (in order of inlet to outlet) 10 mg of Tenax TA, 20 mg of Carbopack X, and 20 mg of Carbopack B, with 15 mg of glass beads between each layer and at the inlet (from Sigma-Aldrich); prior work (Gentner et al., 2012) used a trap composition and analytical system similar to this instrument to sample compounds between C5 and C14. A custom LabVIEW program (National Instruments) operates the instrument for automated sample collection and analysis, with the sample collected for 54.5 min of each hour (total sample volume: 3.8 L). Following sample collection, the trap is thermally desorbed under a helium backflush at 140±10 ∘C for 5.5 min, transferring analytes through a heated 6-port valve (150 ∘C) to the head of the gas chromatography column in a GC oven (Agilent 7890B) with a helium flow rate of 5.5 sccm. GC analysis begins at the end of thermal desorption and proceeds throughout the subsequent sample collection, enabling hourly sample collection and analysis. Analytes are separated using a mid-polarity GC column (Rtx-624, 60 m × 0.32 mm × 1.8 µm, Restek Inc.) and detected by a flame ionization detector (FID). Sample flow is measured by a mass flow controller (MFC1 in Fig. 1, Alicat Scientific), and GC flow is controlled by an electronic pressure controller (EPC in Fig. 1) on board the GC. Ultrapure hydrogen and helium are provided from compressed gas cylinders (5.0 grade, AirGas) as FID fuel gas (H2), FID makeup gas (He), and GC carrier gas (He). Air for the FID is generated on-site at 30 psig with a zero-air generator (Series 7000, Environics, Inc.).
A major advantage of deploying a GC-FID in a field setting is the limited required maintenance. The most frequent maintenance required by the system is the replacement of ozone filters every 4–6 weeks. The system also requires hydrogen and helium gas tanks, which last for roughly 6–8 months (though the former could be generated on-site). GC components (traps, columns) require little to no replacement over the time period reported here under normal operation. The oilless vacuum pump used to pull samples suffers somewhat from constant use and overheating in the warmest months of the year and therefore had to be replaced after ∼ 12 months.
2.2 Calibration and compound identification
For calibration, the sample inlet is overblown with ∼1400 sccm zero air from a zero-air generator, optionally mixed with a multi-component calibrant (Apel-Riemer Environmental Inc.) at one of four different flows (generating four different mixing ratios of calibrant mixtures). A calibration sample occurs each seventh hour, rotating between zero air only, a calibrant at a fixed “tracking” mixing ratio, and a calibrant at one of three other mixing ratios. The composition and pure volume mixing ratio of the multi-component calibrant are provided in Table S1 (in brief: 40.3 ppb isoprene, 4.35–17.60 ppb monoterpenes and sesquiterpenes) and diluted into zero air at flows of 10, 25, 50, and 100 sccm to generate dilutions of approximately 140, 60, 30, and 15 times respectively. Estimated limits of detection for isoprene, isoprene oxidation products, monoterpenes, and sesquiterpenes are 20, 4.3, 2.2, and 2.7 ppt, respectively, estimated as the mixing ratio that would yield a chromatographic peak with a height three times the standard deviation of the noise in the chromatographic baseline. Mixing ratios reported above these levels have an estimated uncertainty of 15 %, primarily driven by uncertainty in chromatographic integration (Isaacman-VanWertz et al., 2017). In most cases, mixing ratios calculated below these values are either reported as LOD (in cases when peaks were too small to be integrated) or reported as calculated but can be considered to have substantial error.
While an FID provides nearly universal quantification of analytes as a function of their carbon content (Scanlon and Willis, 1985; Faiola et al., 2012), it does not provide any chemical resolution. To identify analytes in the samples, a mass spectrometer (MS, Agilent 5977) was deployed in October 2019 and September 2020 in parallel with the FID. Retention times of analytes detected by the two detectors were aligned using the retention time of known analytes (e.g., calibrants). Analytes were identified by mass spectral matching with the 2011 NIST MS Library and reported retention indices (NIST Chemical Kinetics Database, 2020). All analytes reported in this work matched the identified compound within the range of reported retention indices and with a cosine similarity of at least 0.85. This parameter is the preferred spectral comparison method of the widely used NIST mass spectral library search program, and previous work has shown that a threshold of 0.85 or greater indicates a high probability of correct identification (Worton et al., 2017; Stein and Scott, 1994). Data were analyzed using the freely available TERN software packaged (Isaacman-VanWertz et al., 2017) within the Igor Pro 8 programming environment (Wavemetrics, Inc.).
a Atkinson et al. (2006). b Paulot et al. (2009). c Atkinson et al. (1990). d Kerdouci et al. (2010). e Pinto et al. (2007). f Pfrang et al. (2006). g Atkinson and Arey (2003). h Corchnoy and Atkinson (1990). i Shu and Atkinson (1994). j Estimated using King et al. (1999). k U.S. Environmental Protection Agency (2012).
2.3 Atmospheric oxidant reactivity and reaction rate calculations
Reactivity of an individual BVOC and/or a BVOC class to the hydroxyl radical (OHR), ozone (O3R), and nitrate (NO3R) is calculated as the sum of the products of the mixing ratio and oxidation reaction rate of each BVOC, i:
Published rate constants (units: cm3 molec.−1 s−1) at 298 k were used where available (Atkinson et al., 2006; Pfrang et al., 2006; Atkinson et al., 1990; Kerdouci et al., 2010; Pinto et al., 2007; Atkinson and Arey, 2003; Corchnoy and Atkinson, 1990; Shu and Atkinson, 1994; King et al., 1999; Pratt et al., 2012; US Environmental Protection Agency, 2012) and were otherwise calculated from the Kwok and Atkinson structure activity relationships, as implemented by the Estimation Program Interface provided by the US Environmental Protection Agency (Kwok and Atkinson, 1995; US Environmental Protection Agency, 2012; King et al., 1999). Rate constants calculated using structure activity relationships are estimated to be within a factor of ∼2 of measured rate constants (King et al., 1999). However, uncertainty of estimated rate constants is not expected to significantly impact calculated reactivity as compounds with the largest contribution to atmospheric reactivity have measured rate constants.
3.1 Temporal trends in BVOC ratios
Observed and quantified BVOCs include isoprene, two isoprene oxidation products, methyl vinyl ketone and methacrolein, 11 monoterpene species, and two sesquiterpene species (McGlynn and Isaacman-VanWertz, 2021). Due to the nature of the sample collection, diterpenes and many oxygenated species other than MVK and MACR are poorly captured. Oxygenated species either have volatilities that are too high for efficient trapping (e.g., methanol) or are removed by the ozone filter (e.g., nopinone). Many of the small, oxygenated compounds that might be expected at this site at moderately high abundance (e.g., methanol, acetone) have low reaction rate constants that imply they likely contribute only minutely to OHR and NO3R and not at all to O3R. The exception may be acetaldehyde, which previous work has been shown to contribute non-negligibly to reactivity (Hunter et al., 2017) but is too volatile to be trapped by the instrument used in this work. A sample chromatogram is shown in Fig. 2. The detected monoterpene species include α-pinene, β-pinene, β-phellandrene, camphene, limonene, tricyclene, α-fenchene, thujene, cymene, sabinene, and γ-terpinene (Table 1). The sesquiterpene species regularly detected include α-cedrene and β-cedrene, but these are generally present at very low mixing ratios. Consequently, we expect that not all sesquiterpenes are captured by this instrument and caution that all reported mixing ratios of sesquiterpenes represent lower bounds.
Daily 24 h averaged mixing ratios of each BVOC class for the measurement period are shown in Fig. 3. Periods with gaps are due to instrument issues, and periods reported as zero are below the limit of detection (LOD). Many species approached the LOD in the fall and winter months due to low temperatures and decreased incoming shortwave radiation as compared to the warmest months of the year (Fig. S1). Isoprene and its oxidation products (Figs. 3a–b) were near or below detection limits from mid-October to late October through early May. Both classes reached their seasonal peak in late July, with an average ± interquartile range of hourly isoprene mixing ratio in the growing season of 2.13±2.99 ppb, and near levels of detection in the non-growing season; uncertainties here and throughout represent the interquartile range about the mean. The average mixing ratio of summed isoprene oxidation products was 0.27(±0.40) ppb in the growing season and 0.02(±0.03) ppb in the non-growing season. Interestingly, the ratio of isoprene oxidation products to isoprene is variable over the course of the measurement campaign. In addition to differences in their oxidation rates, these differences may be due in part to anthropogenic emissions, both through the influence of NOx on isoprene oxidation pathways and the direct emission of MVK and MACR from vehicles (Biesenthal and Shepson, 1997; Ling et al., 2019). The average mixing ratio of summed monoterpenes in the growing season is 0.74(±0.72) ppb and 0.27 (±0.28) ppb in the non-growing season (Fig. 3c). Monoterpenes exhibit a similar high period during the growing season but are present throughout the non-growing season as well. The average of summer sesquiterpene mixing ratios in the growing season was 0.01(±0.01) ppb and 0.01(±0.01) ppb in the non-growing season. Sesquiterpenes, much like monoterpenes, are detected in both the growing and non-growing season. Average mixing ratios of all classes for each season are provided in Table 2.
Diurnal trends in mixing ratios during the growing season (May–October) and non-growing season (November–April) are shown in Fig. 4 for isoprene, summed isoprene oxidation products, summed monoterpenes, and summed sesquiterpenes. All terpene classes exhibited the highest mixing ratios in the growing season (May–October), when temperature and incoming shortwave radiation were highest (Fig. S1). Isoprene and isoprene oxidation products peak in late afternoon hours, as expected due to the light dependence of isoprene (Guenther, 1997; Zimmerman, 1979; Lamb et al., 1987). Isoprene and oxidation product mixing ratios were typically below the limits of detection in the non-growing season, with little clear diurnal pattern. In contrast to isoprene, summed monoterpenes exhibit peak values in the evening hours, which is consistent with previously reported findings (Panopoulou et al., 2020; Davison et al., 2009). Evening peak values were higher in the growing season than in the non-growing season. Additionally, daytime lows lasted for longer periods of time in the growing season than in the non-growing season due to longer daylight hours driving more photolytic reactions with the OH radical and shorter lasting nighttime boundary layers (Davison et al., 2009). Hourly monoterpene mixing ratios ranged between 0.10 and 2.94 ppb throughout the year, with the lowest values occurring in the non-growing season (Fig. 3b).
Sesquiterpene mixing ratios also exhibited peak diurnal mixing ratios in the evening in the growing season. Summed mixing ratios of sesquiterpenes (Fig. 3g and h) include only two species and so represent a lower bound of possible total sesquiterpene mixing ratios. However, the limit of detection for sesquiterpenes is estimated as 2.7 ppt, so other sesquiterpenes are unlikely to be present at mixing ratios significantly higher than this. Measured sesquiterpenes therefore provide some insight into the total mixing ratios of sesquiterpenes. Mean sesquiterpene (i.e., sum of α- and β-cedrene) values were around 0.01(±0.01) ppb in the growing season and exhibited similar diurnal variability to monoterpenes. Outside the growing season, the mean sesquiterpene mixing ratio was 0.01(±0.01) ppb, with little discernable diurnal variability.
3.2 Calculated reactivity with atmospheric oxidants
3.2.1 Calculated OH reactivity
Calculated OH reactivity of total observed terpenes varies seasonally, with a 24 h average summertime peak of ∼27 s−1 and growing season average of 8.48(±10.68) s−1 driven by isoprene (Fig. 5a). Comparatively, the non-growing season OH reactivity average was 0.99(±1.04) s−1. Reactivity of monoterpenes has weaker seasonality with higher values occurring in the growing season, peaking at ∼3 s−1. These values are roughly within the range of previously reported direct measurements of summertime OH reactivity of 1–21 s−1, where measurements were taken below ponderosa and coniferous forest canopies and within the canopy of a coniferous forest (Ramasamy et al., 2016; Nakashima et al., 2014; Sinha et al., 2010), though at the higher end, likely due to the measurements in this work occurring directly within the canopy. While isoprene dominates reactions with OH when present (Fig. 5b), mixing ratios of isoprene and detected sesquiterpenes are negligible in the non-growing season, causing a steep decline in reactivity. Due to the year-round presence of monoterpenes, these compounds become the dominant source of OH reactivity in the non-growing season. Generally, monoterpenes contribute ∼100 % in the non-growing season and ∼ 15 %–35 % of terpene reactivity in the growing season, with isoprene dominating the balance. Detected isoprene oxidation products and sesquiterpenes contribute, on average, <5 % to OH reactivity. While some sesquiterpenes may be below level of detection, sesquiterpenes do not generally have OH reaction rates substantially higher than other more dominant terpenes (Lee et al., 2006) and so are not likely to contribute substantially to OH reactivity.
3.2.2 Calculated ozone reactivity
Calculated 24 h averaged O3 reactivity ranges between s−1 and s−1 (Fig. 6a) and is almost entirely dominated by monoterpenes (Fig. 6b), even during the growing season peak (monoterpenes: ∼70 %), due to the relatively slow reaction rate of isoprene and its oxidation products with ozone. Ozone reactivity decreases in the non-growing season due to both the decline in isoprene and the decrease in monoterpenes. Average ozone reactivity with isoprene in the growing season is () s−1, while in the non-growing season isoprene does not contribute substantially to ozone reactivity (Table 2). Average ozone reactivity with monoterpenes in the growing season is () s−1, while in the non-growing season it is () s−1 The measured isoprene oxidation products and sesquiterpenes are not strongly reactive with ozone and therefore have no significant contribution to ozone reactivity. However, unlike with OH reaction rates, O3 reaction rates of sesquiterpenes are frequently orders of magnitude larger than dominant monoterpenes, so it is possible that low-abundance, highly reactive sesquiterpenes may still contribute non-negligibly to ozone reactivity. Important contributions by low-abundance, highly reactive sesquiterpenes have been previously shown in other environments and cannot be excluded by these measurements (Yee et al., 2018; Ortega et al., 2007; Arnts et al., 2013; Wolfe et al., 2011).
3.2.3 Calculated nitrate reactivity
Calculated nitrate reactivity of all detected BVOCs is shown in Fig. 7a in addition to the monthly average reactivity and the reactivity of the monoterpene class. The amount that each BVOC class contributes to nitrate reactivity is shown in Fig. 7b. Nitrate reactivity of observed BVOCs varies seasonally, with a summertime peak in 24 h averaged reactivity of ∼0.4 s−1 driven largely by monoterpenes. Reactivity of monoterpenes has strong seasonality, with higher values occurring in the growing season, peaking at ∼0.3–0.4 s−1. As in the case of ozone, nitrate reactivity is dominated by monoterpenes due to the slow reaction rates of isoprene and its oxidation products with NO3. Isoprene contributes between 20 %–45 % to nitrate reactivity in the growing season and has a mean hourly average of 0.04(±0.05) s−1. In the non-growing season, isoprene, like isoprene oxidation products and sesquiterpenes, does not contribute to nitrate reactivity. Monoterpenes dominate nitrate reactivity year-round and have a mean hourly average of 0.10(±0.10) s−1 in the growing season and 0.04(±0.04) s−1 in the non-growing season. Unmeasured and minimally detected sesquiterpenes are unlikely to contribute substantially to nitrate reactivity as their reaction rates are typically of the same order of magnitude as α-pinene and isoprene, but they are present at concentrations 10–100 times lower (Yee et al., 2018).
3.3 Isomer composition of monoterpenes
Monoterpenes are detected year-round, but small changes in their compositional breakdown (i.e., the relative contribution of different isomers) lead to important changes in their reactivity and chemistry. Calculated 24 h average monoterpene mixing ratios ranged between 0.10 and 2.94 ppb, with the lowest mixing ratios occurring in the non-growing season daytime and the highest mixing ratios occurring in the growing season nights (as shown in Fig. 4).
Relative contributions from monoterpene isomers are similar for the highest mixing ratio species between the growing and non-growing seasons (Fig. 8a–b). At nearly all times, α-pinene contributes the most, followed by β-pinene, camphene, limonene, and cymene. OH reactivity (Fig. 8c and d) of each isomer roughly follows the distribution of mixing ratios, driven by the relatively narrow range in OH reaction rates for monoterpenes with double bonds (slowest: α-pinene – cm3 molec.−1 s−1, fastest: β-phellandrene – cm3 molec.−1 s−1). There is nevertheless some outsize contribution to OH reactivity by the low-mixing-ratio isomers β-phellandrene and limonene, which react quickly due to the presence of multiple double bonds and contribute twice as much to reactivity as they do to mixing ratio. Together, these two species account for roughly one-third of OH reactivity, the abundant but less reactive α-pinene accounts for another ∼ one-third, and the remaining monoterpenes account for the remainder (mostly β-pinene, camphene, and γ-terpinene). The stability of the mixing ratios and OH reactivity across a year of measurements suggests that the observed distribution of isomers is a reasonable average representation of monoterpenes in this ecosystem. While α-pinene is the dominant isomer by far, its lower reaction rate relative to other isomers suggest that it is not necessarily a good representative proxy species for the broader monoterpene compound class. Instead, a more general quantitative description of the rate at which monoterpenes react with OH (or any other oxidant) would allow a measurement or estimate of bulk monoterpenes to more accurately be converted into an estimate of their impact on reactivity. Correlations between calculated monoterpene oxidant reactivity and detected monoterpene mixing ratio (Fig. S2) suggest a bulk monoterpene reaction rate of cm3 molec.−1 s−1, ∼30 % greater than the reaction rate of α-pinene, and this average rate is relatively temporally stable. It should also be noted that Fig. 8 suggests that OH reaction with faster reacting, polyunsaturated, lower-mixing-ratio isomers is as likely as reaction with α-pinene.
The role of structure in atmospheric reactions is even more apparent and critical when considering the reactivity of monoterpenes with ozone. Despite its relatively low mixing ratio, limonene is the greatest contributor to reactivity with ozone at 59 % and 48 % in the growing and non-growing season respectively due to an ozone reaction rate 8 times faster than that of the more abundant isomers (Fig. 8e–f). Nearly all the rest of ozone reactivity is contributed by the dominant isomer α-pinene (30 % and 41 %), with a minor contribution from β-phellandrene (5 % and 4 %), β-pinene (2 % and 2 %), and γ-terpinene (1 % and 1 %), while the other isomers are either not reactive with ozone (cymene, tricyclene) or react very slowly with ozone (camphene). Though the general breakdown of ozone reactivity is qualitatively similar during both the growing and non-growing seasons, there are significant quantitative differences. Due to the greater contribution of limonene in the growing season compared to the non-growing season, the relative importance of limonene compared to α-pinene increases substantially in the growing season, from 1.3:1 to 2.1:1. In other words, reactions of monoterpenes with ozone, at least in this canopy, are dominated by reactions with limonene, with a smaller but significant contribution from α-pinene. The bulk O3 reaction rate with monoterpenes (i.e., the rate that best converts hourly mixing ratio to reactivity) is cm3 molec.−1 s−1, ∼25 % faster than α-pinene. However, while this average rate is relatively stable across seasons, there are periods in the growing season during which the average reaction rate of monoterpenes is substantially faster, which could have impacts during these periods (Fig. S2). Isomer dependence of nitrate reactivity is somewhere between O3 and OH, with an outsize impact of limonene but with a more even split of reactivity across monoterpenes species. These trends may be explained by the reaction behavior of nitrate. Like the OH radical, nitrate can react with alkenes by either addition to a double bond or abstract a hydrogen, but it has a stronger tendency to add across a double bond, analogous to O3 (Lee et al., 2014; Pfrang et al., 2006). Similar to OH reactivity, limonene contributes an outsized amount to NO3 reactivity in both the growing and non-growing season (26 % and 19 %). However, for nitrate reactivity, α-pinene remains the dominant component, contributing 48 % to reactions with nitrate in the growing season and 59 % in the non-growing season. The average reaction rate of α-pinene is about ∼10 %–20 % faster than the bulk reaction rate of monoterpenes with nitrate radicals (Fig. S2).
Long-term BVOC measurements are imperative for understanding interannual trends in the formation and loss of ozone and SOA and for improving existing models of BVOC emissions and oxidation. These measurements are difficult, however, without robust measurement techniques that do not require significant maintenance. The use of an automated GC-FID adapted to collect air samples makes it possible to do long-term collection of BVOCs in an unmonitored location. Using this method, we have collected and are continuing to measure a range of BVOCs in the canopy of a forest representative of the Southeastern US, with periodic coupling of a mass spectrometer to allow for identification of the species of interest. The relative ease of this method gives it great potential for additional long-term BVOC monitoring sites to be set up in more locations.
From this study we have gained a greater understanding of the seasonality of BVOCs ranging from isoprene, isoprene oxidation products, monoterpenes, and sesquiterpenes. Isoprene is important for OH reactivity, but monoterpenes prevail as the most important BVOC class for ozone and nitrate reactivities. Monoterpenes are observed to be a diverse class of BVOCs with 11 identified compounds detected at the site year-round. While α-pinene is the most dominant species, a few species with lower mixing ratios but high reactivities (particularly limonene and β-phellandrene) were found to be important contributors to atmospheric reactivity. This finding is most evident for ozone reactivity but is also the case for OH and nitrate reactivity. The distribution of monoterpenes is qualitatively stable throughout the year, though some important quantitative differences are observed. Consequently, the distribution measured here may be a useful description of the “typical” monoterpene chemical class observed in mixed, temperate forests. The bulk reaction rates of the monoterpene class with major atmospheric oxidants presented here therefore provide an improved means to estimate the reactions and impacts of monoterpenes in cases where isomer-resolved measurements are not available (e.g., when measured using direct-air-sampling mass spectrometers (Davison et al., 2009; Ghirardo et al., 2010)).
The integrated GC-FID BVOC data used in this work are available through Mendeley Data. The DOI for this dataset is https://doi.org/10.17632/jx3vn5xxcn.1 (McGlynn and Isaacman-VanWertz, 2021).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-21-15755-2021-supplement.
DFM conducted the measurement campaign, completed the data analysis, and led the writing of the manuscript. GIVW supervised the study, designed the measurement campaign, and directed the data analysis and writing of the manuscript. LERB and SEP were instrumental in the upkeep of the measurement site and provided feedback on the manuscript. MTL provided feedback on the manuscript.
Some authors are members of the editorial board of Atmospheric Chemistry and Physics. The peer-review process was guided by an independent editor, and the authors have also no other competing interests to declare.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This research was funded by the National Science Foundation (AGS 1837882 and AGS 1837891). Tower maintenance and operation were supported in part by the Pace Endowment. Deborah F. McGlynn and Laura E. R. Barry were supported in part by Virginia Space Grant Consortium Graduate Research Fellowships. The authors gratefully acknowledge the assistance of Koong Yi, Graham Frazier, and Bradley Sutliff in their support in the upkeep and maintenance of the instrument at Pace Tower. We thank Todd Scanlon for the use of the meteorological data provided in Fig. S1.
This research has been supported by the National Science Foundation Division of Atmospheric and Geospace Sciences (grant nos. 1837882 and 1837891) and the Virginia Space Grant Consortium.
This paper was edited by Andreas Hofzumahaus and reviewed by two anonymous referees.
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