Total OH reactivity over the Amazon rainforest: variability with temperature, wind, rain, altitude, time of day, season, and an overall budget closure
- 1Atmospheric Chemistry and Multiphase Chemistry Departments, Max Planck Institute for Chemistry, 55128 Mainz, Germany
- 2Département Sciences de l'Atmosphère et Génie de l'Environnement (SAGE), IMT Lille Douai, 59508 Douai, France
- 3Empresa Brasileira de Pesquisa Agropecuária (Embrapa) Amazonia Oriental, CEP 66095-100, Belém, Brazil
- 4Instituto Nacional de Pesquisas da Amazônia (INPA), CEP 69067-375, Manaus, Brazil
- 5Biogeochemical Processes Department, Max Planck Institute for Biogeochemistry, 07745 Jena, Germany
- 6Energy, Environment and Water Research Center, The Cyprus Institute, 1645 Nicosia, Cyprus
- anow at: Department of Environmental Science, Policy, and Management, University of California, Berkeley, CA 94720, USA
- bnow at: Hessisches Landesamt für Naturschutz, Umwelt und Geologie, 65203 Wiesbaden, Germany
Correspondence: Eva Y. Pfannerstill (firstname.lastname@example.org)
The tropical forests are Earth's largest source of biogenic volatile organic compounds (BVOCs) and thus also the largest atmospheric sink region for the hydroxyl radical (OH). However, the OH sink above tropical forests is poorly understood, as past studies have revealed large unattributed fractions of total OH reactivity. We present the first total OH reactivity and volatile organic compound (VOC) measurements made at the Amazon Tall Tower Observatory (ATTO) at 80, 150, and 320 m above ground level, covering two dry seasons, one wet season, and one transition season in 2018–2019. By considering a wide range of previously unaccounted for VOCs, which we identified by proton transfer reaction time-of-flight mass spectrometry (PTR-ToF-MS), the unattributed fraction was with an overall average of 19 % within the measurement uncertainty of ∼ 35 %. In terms of seasonal average OH reactivity, isoprene accounted for 23 %–43 % of the total and oxygenated VOCs (OVOCs) for 22 %–40 %, while monoterpenes, sesquiterpenes, and green leaf volatiles combined were responsible for 9 %–14 %. These findings show that OVOCs were until now an underestimated contributor to the OH sink above the Amazon forest.
By day, total OH reactivity decreased towards higher altitudes with strongest vertical gradients observed around noon during the dry season (−0.026 s−1 m−1), while the gradient was inverted at night. Seasonal differences in total OH reactivity were observed, with the lowest daytime average and standard deviation of 19.9 ± 6.2 s−1 during a wet–dry transition season with frequent precipitation; 23.7 ± 6.5 s−1 during the wet season; and the highest average OH reactivities during two dry-season observation periods with 28.1 ± 7.9 s−1 and 29.1 ± 10.8 s−1, respectively. The effects of different environmental parameters on the OH sink were investigated, and quantified, where possible. Precipitation caused short-term spikes in total OH reactivity, which were followed by below-normal OH reactivity for several hours. Biomass burning increased total OH reactivity by 2.7 to 9.5 s−1. We present a temperature-dependent parameterization of OH reactivity that could be applied in future models of the OH sink to further reduce our knowledge gaps in tropical-forest OH chemistry.
The Amazon rainforest, with its area of over 5.8×106 km2, contains more than half of Earth's tropical forests (Morley, 2000), a quarter of global biodiversity (Dirzo and Raven, 2003), and nearly 15 % of terrestrial biomass (Houghton et al., 2001; Bar-On et al., 2018). The Amazon biome is thus of global relevance for cycling of water, energy, carbon and nutrients (Andreae, 2002; Malhi, 2002; Werth, 2002; Aragão et al., 2014). Understanding its interaction with the atmosphere is highly important for understanding global biogeochemical cycles.
The emission of biogenic volatile organic compounds (BVOCs) by vegetation plays a fundamental role in atmospheric chemistry. Global BVOC emissions are, according to recent estimates, a factor of ∼ 6 higher than anthropogenic volatile organic compound (VOC) emissions (Guenther et al., 2012; Sindelarova et al., 2014; Hoesly et al., 2018). Tropical forests are Earth's largest BVOC source, contributing 65 % of the global isoprene emissions and 77 % of the global monoterpene emissions (Guenther et al., 2012; Sindelarova et al., 2014). The relevance of BVOCs for atmospheric processes stems from their high chemical reactivity. Once released to the atmosphere, BVOCs undergo oxidation reactions within seconds to days, mainly reacting with OH radicals, which are formed during the daytime from the ozone photoproduct O1D and water as well as through recycling reactions (Taraborrelli et al., 2012). This oxidation pathway influences regional tropospheric ozone and secondary organic aerosol formation (Palm et al., 2018; Wyche et al., 2014; Hamilton et al., 2013; Goto et al., 2008; Schulz et al., 2018), thereby impacting oxidative stress to ecosystems, as well as cloud formation and global climate (Bates and Jacob, 2019; Scott et al., 2018; Engelhart et al., 2011; Pöschl et al., 2010; Heald and Spracklen, 2015). Additionally, the reaction of BVOCs with OH affects the regional atmospheric oxidation capacity, which in turn controls the residence times of longer-lived greenhouse gases (e.g., CH4) and pollutants (e.g., CO) (Bates and Jacob, 2019; Arneth et al., 2010; Peñuelas and Staudt, 2010).
More than 30 000 different BVOCs are thought to be released from vegetation (e.g., Harley, 2013) including a wide range of chemical classes, such as terpenoids, alkenes, alcohols, aldehydes, and ketones (Guenther et al., 2012). One measurement survey found 264 BVOC species emitted from tropical trees in French Guiana (Courtois et al., 2009). However, for technical reasons, most studies of BVOCs in tropical forests to date have been limited to a modest number of known, abundant species such as isoprene and monoterpenes and few oxygenated compounds (e.g., Yáñez-Serrano et al., 2015; Langford et al., 2010; Rizzo et al., 2010; Kuhn et al., 2007; Karl et al., 2007; Saxton et al., 2007; Rottenberger et al., 2004; Rinne et al., 2002; Kesselmeier et al., 2000).
Therefore, a measure of the combined effect of all VOCs and other OH reactive species in ambient air is necessary for a complete understanding of local atmospheric chemistry and of the OH sink. This directly measurable quantity is called total OH reactivity, and its value determines the OH loss frequency in reciprocal seconds. By comparing to the OH reactivity calculated from all individually measured compounds (termed the speciated OH reactivity), total OH reactivity can reveal the presence of VOCs that were not measured (termed the unattributed or “missing” OH reactivity).
The tropical forests are the regions of the world with the largest total OH reactivities in the air, with modeled annual averages of 30–50 s−1 (Ferracci et al., 2018; Safieddine et al., 2017). Total OH reactivity in Amazonia is thought to be dominated by isoprene and other reactive BVOCs (Nölscher et al., 2016; Safieddine et al., 2017), which are emitted as a function of light and temperature (e.g., Jardine et al., 2015; Kuhn et al., 2004a; Rinne et al., 2002). However, a significant part of tropical rainforest OH reactivity remains unexplained by speciated trace gases measurements (Nölscher et al., 2016; Williams et al., 2016; Edwards et al., 2013) and by usual global atmospheric chemistry models (Ferracci et al., 2018) with unattributed fractions of 5 %–15 % in the wet and 79 % in the dry season (Nölscher et al., 2016). The unattributed fraction of OH reactivity in tropical forests is assumed to be due to unmeasured oxygenated intermediates (Edwards et al., 2013) or to a combination of oxygenated VOCs (OVOCs) and multiple primary BVOCs (Nölscher et al., 2016). Atmospheric chemistry models do not usually consider this additional, unattributed OH sink, with significant implications for the lifetime of the hydroxyl radical and of methane (Ferracci et al., 2018).
In this work, we used comprehensive VOC information, including compounds with uncertain chemical structure measured by proton transfer reaction time-of-flight mass spectrometry (PTR-ToF-MS), for comparison with total OH reactivity for the first time at a tropical rainforest site. The only previous Amazon rainforest reactivity budget exercise was reported by Nölscher et al. (2016) from a smaller 80 m tower. It was based on data from a proton transfer reaction–quadrupole mass spectrometer (PTR-QMS). The PTR-ToF-MS system used in this study is more sensitive and has a significantly higher mass resolution allowing more compounds to be measured. In this way, we have attempted to obtain closure on apportioning OH reactivity and to identify the previously unidentified OH sinks. Presented here are the first measurements of total OH reactivity at the 320 m high tower at the remote Amazon rainforest site ATTO (Amazon Tall Tower Observatory), covering one wet season, one wet–dry transition season, and two dry seasons in 2018–2019. We discuss vertical gradients between 80 and 320 m above the rainforest floor, as well as seasonality and diel cycles of total OH reactivity and its composition. The influence of environmental parameters such as precipitation and biomass burning is investigated, and a seasonal parameterization for total OH reactivity dependence on temperature is developed.
2.1 Study site – Amazon Tall Tower Observatory
The Amazon Tall Tower Observatory (Andreae et al., 2015) is situated ∼ 150 km northeast of Manaus, Brazil, in a dense, non-flooded terra firme (plateau) forest at ∼ 120 m above sea level. The average rainfall at the site reaches its monthly maximum of ∼ 335 mm in the wet season (February to May) and its minimum of ∼ 47 mm in the dry season (August to November) (Pöhlker et al., 2019). The wet–dry transition season covers June to July and the dry–wet transition season December to January (Andreae et al., 2015; Pöhlker et al., 2016). The main wind directions at the site are northeast during the wet season and east during the dry season (Pöhlker et al., 2019). The site is equipped with several towers. The tall tower with a total height above ground level (a.g.l.) of 325 m is located at 02∘08.602′ S, 59∘00.033′ W. It has been in operation since 2018 with continuous measurements of VOCs, ozone, particles, and basic meteorological data. During intensive observation periods, these were complemented by total OH reactivity observations and sampling of VOCs for offline analysis. A walk-up tower (height a.g.l. 80 m) located ∼ 1 km from the tall tower has been equipped with instrumentation for continuous measurements of meteorology, micrometeorology, greenhouse gases, phenology, inorganic trace gases, and aerosol particles since 2012. Maximum canopy top height of the trees surrounding the towers is ca. 35 m.
2.2 Measurement periods
Continuous total OH reactivity measurements were conducted in March 2018 (7 d; 9–15 March 2018), October 2018 (6 d; 20–26 October 2018), June 2019 (13 d; 10–23 June 2019), and September 2019 (5 d; 22–26 September 2019). These campaigns cover several seasons with March in the wet season (median soil moisture at 10 cm depth 0.169 m3 m−3) and September and October in the dry season (median soil moisture 0.160 and 0.161 m3 m−3, respectively). June is part of the wet–dry transition season. However, June 2019 was particularly wet with flooding at the riverbanks in the study region (median soil moisture 0.218 m3 m−3; see Fig. S1).
Total OH reactivity, ozone, and VOC measurement devices shared an inlet system. Measurement heights at the ATTO tall tower were 80, 150, and 320 m a.g.l., each equipped with its own, constantly flushed (15 L min−1) inlet tube which brought air from aloft to a temperature-controlled laboratory container located adjacent to the tower. At the entry of each inlet, a regularly changed polytetrafluoroethylene (PTFE) filter (5 µm pore size) prevented contamination by particles or insects. The non-transparent inlet tubes (outer diameter, 0.5 in. = 1.27 cm; material, fluorinated ethylene propylene) were heated (∼ 45 ∘C) and insulated with flexible elastomeric foam covering. A valve system was constructed to switch between the different heights, beginning with the lowest height at the full hour and switching to the next height every 5 min. Thus, each height was sampled four times an hour. In order to avoid underpressure at the end of the long inlet lines, the laboratory container was downstream of a chemically inert pump with a Teflon membrane (KNF Neuberger, Freiburg, Germany) with a sampling flow of ca. 17 L min−1. The inlet residence time from 320 m was ∼ 80 s. The inlet response time, i.e., the time for all species to reach a steady signal, determined by sampling a calibration gas mixture introduced at the 320 m inlet entrance, ranged between 88 s (for methanol) and 96 s (for acetaldehyde, benzene, trimethylbenzene, methacrolein), with an average of 93 s. Consequently, the data measured in the first 100 s after each valve switch were not included in the data analysis.
2.4 Inlet effects
Due to the length of the inlet tubing of more than 320 m from the top of the ATTO tall tower to the instrumentation, potential sampling losses have to be considered. Losses can be irreversible due to oxidation with ozone or reversible due to interactions with the tubing. The most ozone-reactive VOCs observed in this study are sesquiterpenes, and the sesquiterpene mixture at 80 m a.g.l. and higher was relatively unreactive, as can be seen in the thermodesorption (TD)-gas chromatography (GC)-ToF-MS-derived speciation in Table S1. The most reactive sesquiterpene mixture observed (lowest height, dry season) had an average reaction rate coefficient of cm3 molecules−1 s−1 towards ozone and thus a lifetime of ca. 5.5 h for peak diel ozone concentrations of 17 ppb (dry season). The inlet residence time of 80 s is therefore not considered to be long enough for significant losses in sesquiterpenes. Potential chemical losses due to ozone being present in the inlet tube are thus considered negligible.
VOCs, especially polar compounds, can partition reversibly from the gas phase to Teflon tubing walls (Deming et al., 2019; Pagonis et al., 2017; Liu et al., 2019). This causes a delay in the time profile of the VOCs, similar to the effect a chromatographic column (Pagonis et al., 2017). In consequence, concentration peaks are smeared and broadened, which causes an underestimation of observed concentrations (Deming et al., 2019). The ATTO inlet tubing was constantly flushed even when not being sampled, so surfaces were assumed to be saturated or near equilibrium so that inlet interactions were minimized. We determined inlet losses in peak concentrations from the 320 m inlet to the instrument by introducing a calibration gas mixture from the top of the tower. The losses in peak concentration ranged between 11 % and 30 % for all substances in the calibration mixture. We did not correct final data for inlet losses in order to keep VOC and total OH reactivity data, which were both measured from the same inlet, comparable (inlet loss correction for total OH reactivity would change according to its composition, which is not entirely known) and because loss fractions for substances not included in the calibration mixture are not known. This means that the total OH reactivity and VOC concentrations observed in this study may be underestimated in their peak values and smeared towards later times of the day but that the overall daytime sum should be unaffected.
2.5 Total OH reactivity, trace gas, and black carbon measurements
During all four campaigns, total OH reactivity was determined using the comparative reactivity method (CRM; Sinha et al., 2008). The method was recently compared to other OH reactivity measurement devices (Fuchs et al., 2017) and has been applied in various regions of the world (Yang et al., 2016). Briefly, CRM uses the known OH reactivity of a pyrrole gas standard (Westfalen AG, Münster, Germany) and compares it with the reactivity of all compounds found in ambient air in a competitive reaction. OH radicals are created inside a glass reactor by flushing humidified nitrogen (6.0 grade, Westfalen AG, Münster, Germany) over a Hg–Ar UV lamp (LOT-QuantumDesign, Darmstadt, Germany). CRM uses three different modes: C1 (OH scavenger + pyrrole + UV light at ∼ ambient humidity), C2 (OH + pyrrole, ambient humidity), and C3 (ambient air + pyrrole + OH) level. For a more detailed description, see Sinha et al. (2008) and Michoud et al. (2015).
In our study, the C2 level was measured for 15 min at the beginning of each hour, followed by 45 min of C3 measurement. C1 level determinations and calibrations with a pyrrole gas standard (Westfalen AG, Münster, Germany) were performed at least twice during each campaign. The C1 level was typically 68 ± 1 ppb (parts per billion = nmol mol−1). The system was operated at a pyrrole OH ratio of 2.76 ± 0.23 (average ± standard deviation). As is typical in the CRM, this ratio deviates from the pseudo-first-order conditions assumed in the CRM equation (Sinha et al., 2008). Therefore, a correction had to be applied (see Sect. 2.5).
The pyrrole mixing ratio was monitored by a proton transfer reaction–quadrupole mass spectrometer (PTR-QMS; Ionicon Analytik, Innsbruck, Austria; Lindinger et al., 1998) at . The instrument was operated at 60 ∘C drift temperature, 2.2 mbar drift pressure, 600 V drift voltage, and 137 Td.
Simultaneously, VOC measurements up to were conducted using a PTR ToF mass spectrometer (Ionicon Analytik, Innsbruck, Austria; Jordan et al., 2009), operated at 60 ∘C drift temperature, 3.5 mbar drift pressure, 850 V drift voltage, and 120 Td. The instrument was calibrated with a gravimetrically prepared multicomponent VOC standard (Apel-Riemer Environmental Inc., Colorado, USA) once during each campaign. Diiodobenzene was continuously fed into the sample stream for mass-scale calibration. The time resolution of the measurement was 20 s. The mass resolution (full width at half maximum) ranged between 3000 and ∼ 3500. A complete list of the trace gases measured by PTR-ToF-MS can be found in Table S1.
CO and methane were sampled at the walk-up tower at 80 m a.g.l. using a cavity ring-down spectroscopy instrument (Picarro Inc., Santa Clara, California, USA). From preliminary CO and methane measurements at the 320 m tower, vertical gradients were taken to calculate approximate concentrations for 150 and 320 m from the 80 m observations. For CO, 10 and 30 ppb were subtracted from the 80 m values to derive lower-limit mixing ratios for 150 and 320 m, respectively. Methane values measured at 80 m were assumed to be valid for all heights, because the small height-related differences observed are not on an order of magnitude that affects OH reactivity (Botía et al., 2020).
For monoterpene and sesquiterpene speciation, air samples were collected on adsorbent filled tubes equipped with ozone scrubbers at different heights on the ATTO tall tower (Zannoni et al., 2020a). Sampling occurred every 3 h for 2 weeks at 80 and 150 m (March 2018) and every hour for 3 d at 80, 150, and 320 m (October 2018). Samples were analyzed in the laboratory by a TD-GC-ToF mass spectrometer (Markes International, Llantrisant, United Kingdom).
Measurements of black carbon mass concentrations were obtained at the 325 m inlet of the ATTO tall tower using a multi-angle absorption photometer (MAAP; model 5012, Thermo Fisher Scientific, Waltham, Massachusetts, USA), as described in Holanda et al. (2020).
2.6 Total OH reactivity data analysis
CRM data analysis and corrections were conducted following the procedures described in Pfannerstill et al. (2019). The humidity correction amounted to an average of 5 % and the ozone correction to an average of 2 % of the measured OH reactivity. An NO NO2 correction was not performed due to the low NOx levels at the site (Pfannerstill et al., 2018; Wolff, 2015) with maximum NO and NO2 mixing ratios of 0.36 and 0.62 ppb in the dry season (October 2018), respectively. The correction for pseudo-first-order deviation was derived from tests using propene, isoprene, and propane, resulting in a weighted correction factor in dependence on the alkene fraction in calculated OH reactivity and the pyrrole OH ratio (Eq. 1):
where F is the total correction factor and the weighted, pyrrole OH-dependent correction factors were × pyrrole OH + 2.98 and F2=0.63 for March 2018, × pyrrole OH + 4.73 and pyrrole OH + 1.55 for October 2018, pyrrole OH +4.50 and F2= 0.94 for June 2019, and pyrrole OH +3.05 and F2=0.94 for September 2019. Xalkenes is the speciated OH reactivity fraction of alkenes. This correction increased OH reactivity by a factor of 1.12 ± 0.10 (average ± standard deviation).
The dilution of ambient air with humidified nitrogen was accounted for with a dilution factor of 1.3.
The 5 min detection limits (LODs), derived from the 2σ standard deviation of background (C2) measurements, ranged between 4.0 and 7.0 s−1 (depending on PTR-QMS performance). Total uncertainty (1σ) of the measurements was 35 % (median), with a precision of 16 %–41 % over 5 min depending on the quantity of reactivity.
2.7 Calculated OH reactivity from individually measured compounds (speciated OH reactivity)
Table S1 lists the 83 VOCs and 3 inorganic trace gases and their reaction rate constants considered for calculating speciated OH reactivity. The speciated OH reactivity is the sum of the OH reactivities attributed to individual (measured) trace gases (Eq. 2):
Contributions of VOCs and inorganic trace gases (where [VOC] is their respective concentrations in molecules cm−3) to OH reactivity (R in s−1) are calculated using the gas-phase reaction rate constants (kVOC+OH in cm3 molecule−1 s−1) of the respective compounds with the OH radical. The difference between the sum of individual trace gas contributions to OH reactivity and measured total OH reactivity is termed “unattributed” or missing OH reactivity. Out of a total of 86 chemical species that were considered for the calculation of speciated reactivity here, 13 VOCs (specified in Table S1), including the most important known contributors to OH reactivity in the tropical forest, were calibrated with gas standards and therefore have low uncertainties in their concentrations as well as in their reaction rate coefficients (5 %–15 %). A further 70 exact masses (specified in Table S1) monitored by PTR-ToF-MS were attributed to molecular formulae, and their concentrations were derived using a theoretical approach (Lindinger and Jordan, 1998), which has an uncertainty of ca. 50 %. In cases where several chemical structures could be attributed to the measured mass, an average of the known reaction rate coefficients with OH was used for calculating the speciated OH reactivity. In the few cases where rate coefficients were unknown in the literature, the rate coefficient of a VOC with comparable functional groups was applied (see Table S1). Due to the occasional large differences in rate coefficients between possible structures, the uncertainty in the reaction rate coefficients kVOC+OH is estimated to be 100 %. The uncertainty in the resulting speciated (i.e., calculated) OH reactivity depends on the fraction of gas-standard-calibrated compounds in the ambient air at any given point of time and varied between 15 % and 65 %, with an average (± standard deviation) of 36 % ± 9 %. The relative composition of the total monoterpenes and sesquiterpenes measured by PTR-ToF-MS was derived from TD-GC-ToF-MS data as specified in Table S1.
Periods influenced strongly by biomass burning were identified using an index defined as the 3* acetonitrile mixing ratio in parts per billion + black carbon mass in micrograms per cubic meter. If this index was > 1 in the dry season or > 0.75 in the wet and transition season, the respective data point was defined as strongly biomass burning influenced, whereas other data points were categorized as low biomass burning influenced. This index was tested against the pristine-conditions index PRBC ∪ CO from Pöhlker et al. (2018) for March 2018. In this period, ∼ 80 % of the data points were categorized in the same way by both indices.
3.1 Vertical, diel, and seasonal variation in total OH reactivity
3.1.1 Total OH reactivity profiles and diel cycles
Profiles of total OH reactivity between 80 and 320 m a.g.l. at the ATTO tall tower are shown for different seasons and times of the day in Fig. 1. Generally, noontime OH reactivity was higher in the dry seasons than in the wet or transition seasons, which is consistent with earlier studies at lower heights (Nölscher et al., 2016). The overall lowest noontime (11:00–15:00 LT (local time)) OH reactivity average was observed with 23.2 s−1 at 80 m during the wettest period (June 2019, Fig. S1), and the highest noontime average was observed with 39.4 s−1 during the driest period of measurements (September 2019).
Nighttime (00:00–05:00 local time) averages were lower, at between 14.1 and 20.2 s−1. Interestingly, the noontime–nighttime difference was with 12.4–22.5 s−1 much larger in the dry season than in the wet season (6.7 s−1). The nighttime values appear to be relatively consistent over the different measurement periods, whereas the noontime values are subject to larger seasonal differences. This is probably related to larger temperature differences between day and night in the dry season (see Sect. 3.3.1).
In all seasons, there was a negative vertical gradient of OH reactivity towards higher levels around noon. This is expected, because noon and early afternoon is the time when the vegetation reaches its emission maximum (Sarkar et al., 2020). Reactive VOCs emitted by the vegetation become oxidized to less reactive compounds while they are transported aloft (see Sect. 3.2). The vertical OH reactivity gradient was strongest in the driest period observed (September 2019; noontime gradient −0.026 s−1 m−1; see Fig. S3), with a maximum difference between 80 and 320 m of 6.8 s−1, and weakest in the wet season (March 2018; noontime gradient −0.005 s−1 m−1), with a maximum difference between 80 and 320 m of 1.3 s−1. The dry season vertical gradient was here approximately a factor of 4 lower than the OH reactivity gradient observed directly above the rainforest canopy from 24 up to 80 m in the 2013 dry season (Nölscher et al., 2016). This behavior was also observed in aircraft measurements of isoprene and monoterpenes, where vertical gradients inside the boundary layer above the rainforest decreased with height (Karl et al., 2007; Kuhn et al., 2007). In the wet season, the gradients measured here were comparable to those seen directly above the canopy in the 2013 wet season (Nölscher et al., 2016).
Between 80 and 320 m, the variability in the data (shown as standard deviations) was often as large as the gradient (Fig. 1). This suggests that turbulent mixing above the forest was often strong enough to transport reactive VOCs to higher levels faster than the majority of the reactants could become oxidized to less reactive species. This observation reflects the well-mixed nature of air above rainforest canopies in the daytime (Freire et al., 2017; Fuentes et al., 2016).
At nighttime, vertical gradients in total OH reactivity were barely discernable. The data suggest a slightly lower (by up to 1.8 s−1) OH reactivity at the lowest observation level (80 m) than at 150 m and/or 320 m in all observation periods except September. The OH radical, the dominant VOC sink, is not available during the night to any significant degree, although some can be generated by the reaction of ozone with terpenoids (Pfeiffer et al., 1998; Aschmann et al., 2002; Taraborrelli et al., 2012). Potentially, deposition to the surfaces of the forest canopy or to the soil becomes a relevant VOC sink visible in the 80 m values at night, while surfaces for dry deposition are less available at higher altitudes. VOC deposition on ecosystems and plants and even uptake to the cuticles has been observed in the past (Niinemets et al., 2014; Karl et al., 2010; Park et al., 2013; Langford et al., 2010; Cappellin et al., 2017). A study conducted at the ATTO site found strong nighttime canopy deposition of monoterpenes which was a function of surface wetness (Yáñez-Serrano et al., 2018). Deposition can thus partly explain the weaker vertical gradients in the wet season, when the overcast conditions led to weaker irradiation and therewith lower OH levels, while deposition continued or was even increased due to precipitation. Soils can act as an additional VOC sink (Tang et al., 2019; Pegoraro et al., 2005; Cleveland and Yavitt, 1997).
Total OH reactivity diel cycles (Fig. 2) reflect the typical diurnal behavior of BVOC concentrations previously measured in the rainforest (Langford et al., 2010; Yáñez-Serrano et al., 2015; Rizzo et al., 2010), which is broadened towards the evening hours in comparison to emission fluxes (Sarkar et al., 2020; Kuhn et al., 2007). Sunrise was around 06:00 local time (LT) and sunset around 18:00, independent of the season. In the mornings, OH reactivity started to increase in the 1–2 h following sunrise, in parallel with temperature. The OH reactivity maximum occurred between 12:00 and 15:00 LT. At the end of the day, OH reactivity decreased with PAR (photosynthetically active radiation) but, following the pattern of temperature more closely than that of PAR, did not reach nighttime levels until 2–4 h after sunset. Note that the OH reactivity maximum may be a lower limit due to inlet-related smearing of peak concentrations (Sect. 2.4).
Minimum total OH reactivity values were generally observed in the early morning before sunrise, coinciding with the lowest diel temperatures. The dependence of OH reactivity on temperature is discussed in more detail in Sect. 3.3.1.
In both dry seasons and the wet season, a second peak of OH reactivity, smaller than the noontime maximum, occurred during sunset. Potentially, this was related to a combination of a transport effect and terpenoid emissions spread out until the evening (Pfannerstill et al., 2018).
The differences in OH reactivity diel cycles between heights were often within the standard deviation of diel hourly averages, usually with slightly higher values at 80 m during the day as discussed above.
3.1.2 Total OH reactivity seasonality
The lowest temperatures and PAR values were observed during the wet season (March; hourly diel maxima 27.4 ∘C and 1166 µmol m−2 s−1), followed by the wet–dry transition season (June: 31.5 ∘C, 1955 µmol m−2 s−1), and the two dry season periods (October, 33.1 ∘C, 1987 µmol m−2 s−1; September, 30.6 ∘C, 2230 µmol m−2 s−1). Surprisingly, we observed the lowest daytime OH reactivity in the wet–dry transition season (June) with a diel hourly maximum at 80 m of 24.0 s−1 when temperature and irradiation were higher than in March (28.2 s−1). However, as mentioned previously, the June 2019 transition season was particularly wet with frequent rainfall and with a higher soil moisture than March 2018 (Fig. S1). These conditions appear to have influenced BVOC concentrations, e.g., due to root inundation (Bracho-Nunez et al., 2012) or by a potential delay of leaf flushing that usually starts in many trees during the wet-to-dry transition season (Lopes et al., 2016), which would have influenced leaf phenology, another driver of tropical BVOC emissions (Alves et al., 2018; Wei et al., 2018). Also, wet deposition was enhanced in June, contributing to reduced OVOC concentrations (see Sect. 3.2). Influence of rainfall on OH reactivity is further discussed in Sect. 3.3.3. During the dry seasons, the diel hourly maxima of OH reactivity were 35.9 and 41.5 s−1 for October 2018 and September 2019, respectively. The larger daytime OH reactivity in September was accompanied by higher PAR than in October.
In contrast to the daytime values, the nighttime OH reactivity in September 2019 was significantly lower than in October 2018. One potential reason is found in enhanced nighttime ozone levels in September 2019, when nighttime average ozone mixing ratios were 39 % (4.3 ± 1.7 ppb) higher than in October 2018 (Fig. 3). Ozone is a direct sink for terpenoid compounds but also generates secondary OH from the reaction with terpenes and sesquiterpenes (Pfeiffer et al., 1998; Aschmann et al., 2002; Taraborrelli et al., 2012). This might have led to a larger nighttime VOC loss in September 2019. However, other potential explanations such as inter-annual differences in nighttime deposition cannot be ruled out.
The seasonal behavior in total OH reactivity observed here, with a maximum in September and a minimum in June, is consistent with satellite-derived isoprene observations from 2010 to 2011 (Alves et al., 2016). A comparison of the values presented here with OH reactivity measurements made in 2013 at the same site (at 79 m a.g.l. at the walk-up tower; Nölscher et al., 2016) shows very similar values between June 2013 and June 2019. In March 2013, the observed values were lower and in September 2013 they were higher than in the same months in 2018–2019. A potential reason for these differences could be inter-annual variability. For example, March 2018 was less humid than March 2013 with median soil moisture of 0.169 m3 m−3 vs. 0.233 m3 m−3, and it was relatively strongly influenced by biomass burning (Sect. 3.3.4). As discussed above, OH reactivity is generally higher under drier rainforest conditions (Fig. S1). Other factors not monitored, such as herbivore activity, can vary strongly between years (Velasque and Del-Claro, 2016) and can elicit the release of certain BVOCs that might contribute to inter-annual differences. Additionally, the VOC composition measured at the same height can differ between the walk-up tower used in 2013 and the tall tower used in 2018–2019 due to local emissions (Zannoni et al., 2020a). The walk-up tower is built directly adjacent to trees, which might increase the influence and amount of very local, momentary BVOC emissions that could have led to the higher OH reactivities in September 2013, while the tall tower has a much larger footprint (Pöhlker et al., 2019) and is built on a small clearing.
3.2 OH reactivity budget
3.2.1 OH reactivity speciation overview and unattributed reactivity
In forested environments, the total OH sink is generally less well understood than in urban air masses (Yang et al., 2016; Williams and Brune, 2015; Zannoni et al., 2017). Previous total OH reactivity observations in tropical forests revealed large unattributed OH reactivity fractions of 50 %–79 % (Nölscher et al., 2016; Edwards et al., 2013; Sinha et al., 2008). The unattributed fraction in these past studies was largest in the dry season at night (around 80 %), while it was smallest in the wet season around noon (5 %–50 %) (Nölscher et al., 2016). However, the number of trace gases included in these earlier investigations was restricted to only 15 to 19 species due to technical limitations. As the unattributed fraction depends on the number and relevance of trace gases included, we investigate here how well we can explain the OH reactivity budget by measuring a larger number of VOCs by PTR-ToF-MS. As a comparison to a previous OH reactivity study at the ATTO site, the compounds included in Nölscher et al. (2016) were marked with a “*” in Table S1.
We used 83 VOCs (for a complete list see Table S1) monitored by PTR-ToF-MS to compare with measured total OH reactivity. The VOCs which were calibrated by a theoretical approach (see Sect. 2.6 and Table S1) contributed between 29 % and 39 % of total OH reactivity. The unattributed fraction resulting from the inclusion of both gas-standard-calibrated VOCs and those calibrated by the theoretical approach was usually in the range of the measurement uncertainty (Fig. 4) and within the between-day variability (shown as standard deviation). Applying a more comprehensive VOC measurement technique, we can thus close the OH reactivity budget within the uncertainty. The unattributed fraction was independent of measurement height (Fig. S2); therefore data from 80 m are shown in Fig. 4 as a representative example.
The PTR-ToF-MS measurements revealed that an unexpectedly large fraction of total OH reactivity above the rainforest was due to oxygenated VOCs (OVOCs). Only five OVOC species (methanol, acetaldehyde, acetone, methyl ethyl ketone, sum of methacrolein + methyl vinyl ketone + ISOPOOH) could be monitored in previous studies, amounting to 10 %–15 % of speciated and 4 %–5 % of total OH reactivity (Nölscher et al., 2016). A model has subsequently attributed 19 % of Amazon OH reactivity to OVOCs (Safieddine et al., 2017). In addition to the aforementioned gas-standard-calibrated OVOC species, here we include OVOCs calibrated by a theoretical approach. As a result, we observe a higher OVOC-attributed speciated OH reactivity fraction of 34 %–46 % (22 %–40 % of the total OH reactivity), attributed to 45 OVOC species. These include reactive oxygenates that were not included in earlier observations, e.g., 3-methyl-furan (an isoprene oxidation product; Atkinson et al., 1989; Jardine et al., 2013), and monoterpene oxidation products with the chemical formula C9H14O (identified as nopinone and sabinaketone by TD-GC-ToF-MS). Our findings support modeling results of Taraborrelli et al. (2012) which predicted that half of the OH reactivity associated with the presence of isoprene would be due to its oxidation products.
The smallest daytime average OVOC OH reactivity at 80 m a.g.l. (4.2 s−1, 21 % of the total) was observed in the rainiest observation period (June 2019, with an average of 4.4 mm of rain per day), in contrast to the highest average in the dry season (October 2018, 0.7 mm of rain per day) with 8.8 s−1 (31 % of the total). This difference can be explained by a lower OVOC formation rate associated with lower irradiation and a higher tendency for wet deposition of OVOCs associated with the higher precipitation rates in June (Langford et al., 2010).
In this study, isoprene accounted for 38 %–46 % of calculated and 23 %–43 % of total OH reactivity, and it was thereby the single chemical species with the largest contribution to OH reactivity. However, this percentage is lower than the 70 % of calculated OH reactivity found at the Z14 station in central Amazonia (Karl et al., 2007) and the 54 %–70 % of calculated OH reactivity inside the canopy at the ATTO site in 2013 (Nölscher et al., 2016). However, Nölscher et al. (2016) already noted that isoprene accounted for only ∼ 20 % of the total OH reactivity during dry-season afternoons.
Our PTR-ToF-MS measurements also revealed several directly emitted BVOC species which were not included in earlier rainforest OH reactivity studies – e.g., the sum of sesquiterpenes, oxygenated (e.g., citronellol, thymol) and aromatic monoterpenes (e.g., p-cymene, cymenene), and several green leaf volatiles (GLVs; e.g., hexenol, hexenyl acetate, hexanal), some of which are highly reactive towards OH. In total, we found 31 BVOCs that are probably direct emissions according to the literature, which is a large number compared to previous rainforest OH reactivity studies but a small number in comparison with a study that found 264 different VOCs in the emissions of tropical trees directly measured at the leaf/bark level (Courtois et al., 2009). However, the most reactive among the directly emitted BVOCs are not expected to live long enough to reach the 80 m and higher observation platforms.
The sum of GLVs contributed 5 %–8 % of total OH reactivity. Monoterpenes and sesquiterpenes contributed on average 2 %–7 % and 0.1 %–0.9 % of total OH reactivity, respectively. In summary, all groups of primary BVOCs except for isoprene were smaller OH sinks than the summed OVOCs. However, it has to be noted that some OVOCs can be primary plant emissions and do not necessarily have to be the result of atmospheric oxidation processes (Harley et al., 2007; Schade and Goldstein, 2002; Rottenberger et al., 2004; Bracho-Nunez et al., 2013; Niinemets et al., 2014). Even isoprene oxidation products can be directly emitted to a certain extent (Jardine et al., 2013).
The OH reactivity of CO and methane (grouped as “inorganics”, Fig. 4) amounted to 3 %–4 % of the total, with CO mainly varying under biomass burning influence. The OH reactivity attributed to aromatics and sulfur- and nitrogen-containing VOCs (grouped under “others”) was small with 0 %–1 % of the total.
The three individual species that contributed most to daytime OH reactivity were in both dry seasons and in the transition season isoprene > sum of methacrolein (MACR) + methyl vinyl ketone (MVK) + ISOPOOH > monoterpenes. In the wet season they were isoprene > sum of MACR + MVK + ISOPOOH > sum of hexenol + hexanal.
Previous studies explained unattributed OH reactivity fractions in the rainforest with a mixture of unmeasured primary BVOCs (e.g., green leaf volatiles, sesquiterpenes) and BVOC photooxidation products (Nölscher et al., 2016) or with oxidation products alone (Edwards et al., 2013). Edwards et al. (2013) created a box model to account for unattributed OH reactivity in a Southeast Asian rainforest, which included ∼ 900 oxidized intermediates that contributed 47 % of the calculated OH reactivity. Our data, with 23 %–43 % of total OH reactivity attributed to 45 OVOC species and ∼ 10 % to several previously unaccounted for primary BVOCs (including green leaf volatiles, oxygenated and aromatic monoterpenes, and sesquiterpenes), indicate that previously unattributed OH reactivity fractions were due to both primary BVOCs and oxidation products, with oxidation products dominating. Our analysis shows that the previously unattributed OH reactivity cannot be explained by a few key species but rather that a multitude of relatively small contributions, in particular from OVOC, explain the sum of OH reactivity. As illustrated in Fig. S4 and Table S1, no VOC exceeds an average OH reactivity of 1 s−1 except for both isoprene and its oxidation product measured on (MVK/MACR/ISOPOOH).
Assuming that the remaining unattributed OH reactivity fraction here is significant despite being within the measurement uncertainty (Fig. 4), 7 %–35 % of the total OH reactivity (seasonal averages) remains unexplained here. This fraction was lowest in the dry season afternoons (4 %–11 %) – interestingly, the time of the day with the largest unattributed OH reactivity in Nölscher et al. (2016). This is also the time with the largest OVOC reactivity, which explains why closure could be significantly improved for the afternoons here compared to in previous studies.
Over all seasons, the unattributed fraction was largest and most variable in the early morning (Fig. 4, 28 %–39 %). This is when vegetation starts its diurnal photosynthetic activity with the largest CO2 uptake and stomatal conductance of the day (Pfannerstill et al., 2018). At this time of the day, emission of primary BVOCs from storage pools and from buildup within the leaf while the stomata are closed is likely, suggesting that part of the remaining unaccounted for OH reactivity in this work could be due to direct plant emissions. The number of different VOCs emitted by vegetation is potentially much larger than the number we were able to measure (Courtois et al., 2009). A peak in sesquiterpene mixing ratios co-occurs with the early-morning peak in unattributed OH reactivity (Zannoni et al., 2020b), perhaps indicating a common source of the sesquiterpenes and the unidentified reactants.
As the PTR-ToF-MS is not able to separate or identify all OVOC species and misses unstable intermediates, further unmeasured secondary oxygenates could be responsible for the remaining unattributed OH reactivity in this study. The fact that the unattributed OH reactivity fraction appears to be independent of altitude (Fig. S2) may be an indicator for long-lived OVOC species contributing to the remaining unattributed fraction. However, it has to be noted again that the uncertainty in the measurement was generally larger here than the unattributed fraction.
3.2.2 Vertical and diel trends in OH reactivity speciation
OH reactivity speciation at the ATTO tall tower reveals height-related trends (Fig. 5a, b; Table 1).
In all seasons during the daytime, the OH reactivity contribution of directly emitted BVOCs (isoprene, terpenoids) decreased with height (e.g., for isoprene from 51 % at 80 m to 39 % at 320 m in October 2018), while the fraction of oxidation products, i.e., OVOCs, increased (e.g., from 31 % to 39 % in October 2018). Also, the number of oxygen atoms in OVOCs increased with height, while the OH reactivity fraction of non-oxygenated CxHy VOCs decreased, as shown in Fig. 6a–d. This is due to the increasing average photochemical age of the air mass with height, which increases the abundance of OVOCs relative to primary BVOCs such as isoprene (Karl et al., 2009). Figure 6e illustrates the increasing photochemical age of air towards the top of the tower by showing ratios of isoprene and monoterpene oxidation products vs. precursors. The monoterpene oxidation products monoterpenes (MTO MT) ratios are generally lower than the isoprene oxidation products isoprene ratios (IsopO Isop) because the oxidation of isoprene with OH is faster than that of the average monoterpene. For the ATTO monoterpene mixture as identified by TD-GC-ToF-MS (Table S1), the ratio of k(OH + isoprene) k(OH + monoterpenes) was around 1.38. In agreement with this difference in OH oxidation velocity, the ratio (IsopO Isop) (MTO MT) was between 1.01 (80 m, rainy season) and 2.34 (80 m, dry season).
Figure 6 also shows seasonal variability in the oxidation state and oxidation product precursor ratios. Fractions of highly oxygenated VOCs (Fig. 6a–d) and oxidation product precursor ratios (Fig. 6e) were lowest in the rainy season (March 2018) and higher in the transition season (June 2019) and dry seasons (October 2018, September 2019). This seasonality in ratio corresponds to the seasonal differences in solar irradiation with a higher OH production rate in the dry season and thus increased photochemistry. The low MTO MT ratio in September 2019 was due to similar concentrations of oxidation products despite higher monoterpene concentrations than in June 2019.
In order to compare the relevance of the different VOC classes for the carbon cycle with their relevance as OH sinks, Fig. 5c and d show carbon concentration. If the carbon concentration is considered instead of the OH reactivity, the fraction of OVOCs (daytime 52 %–66 %) dominates over the isoprene fraction (daytime 12 %–27 %) at every height. The intense solar irradiation, high temperature, and humidity in the tropical rainforest environment lead to rapid conversion of primary BVOCs to secondary oxygenated compounds (Karl et al., 2009). Our results indicate that a considerable part of the BVOCs directly emitted by vegetation is already oxidized when reaching 80 m, but since oxidation of terpenoids decreases their reactivity (Nölscher et al., 2014), their contribution to the total OH sink is smaller than their contribution to total carbon concentration (Fig. 5c, d) or their contribution to the total VOC mixing ratio (Fig. 5e, f).
At nighttime, the composition of OH reactivity was shifted towards OVOCs. They accounted for 23 %–40 % of the total nighttime OH reactivity, while isoprene contribution decreased to 19 %–36 %. This reflects that OVOCs produced during the day have longer lifetimes than isoprene and therefore are not as efficiently removed from the atmosphere before nightfall. In terms of carbon, the OVOC fraction increases to 57 %–73 % at night.
The positive nighttime vertical gradient towards higher altitudes which is recognizable in total OH reactivity (see Sect. 3.1.1) is more distinct in carbon concentration and mixing ratios (Fig. 5d, f). This supports the conclusion that deposition to the canopy may become a relevant VOC sink at night (see Sect. 3.1.1). The compound group predominantly responsible for the positive upward gradient is OVOCs with a 16 % larger nighttime OVOC reactivity and 23 % larger OVOC mixing ratio at 320 m compared to 80 m (October 2018). With their high polarity and molecular mass, OVOCs are likely to be subject to dry deposition to surfaces.
3.3 Dependence of OH reactivity on environmental parameters
Total OH reactivity observed above the rainforest can change due to variation in several environmental factors, e.g., the release of BVOCs from storage compartments or after in situ de novo production from vegetation, transport processes to the point of observation, other meteorological factors such as wind and rain, or biomass burning. In this section we investigate how total OH reactivity changed with these factors, in the hope of gaining insights that can be used in modeling Amazon forest OH reactivity.
Diel cycles (Sect. 3.1) showed that the patterns of total OH reactivity and ambient temperature were similar. Plant BVOC emissions are known to depend on temperature and are thought to provide, among other advantages, a heat stress coping mechanism (e.g., Penuelas and Munne-Bosch, 2005; Sharkey et al., 2008). As illustrated in Fig. S4 and by the color scaling in Fig. 7, higher temperature and OH reactivity often co-occurred with higher PAR because temperature is driven by PAR in the daytime. PAR is a driver of reactive emissions in the rainforest (Kuhn et al., 2004a; Jardine et al., 2015). However, there is a PAR-independent temperature dependence visible at PAR = 0, i.e., during the night, and the correlation of OH reactivity with PAR was weaker than with temperature (Figs. 7, S5). Air temperature can serve as a proxy for the combined effects of direct light- and temperature-dependent emission as well as transport, which all influence observed total OH reactivity. Thus, in this simplistic approach, we assume that any PAR- and transport-related influences on OH reactant levels at the ATTO tall tower will be captured indirectly by using a temperature-dependent parameterization. This is why we chose to parameterize OH reactivity based on temperature rather than on PAR. The relationship is not intended to be used as an emission algorithm but to facilitate comparison with model-generated results.
Since total OH reactivity above the rainforest is dominated by primary BVOCs (Sect. 3.2), we investigate here the dependence of total OH reactivity measured at 80 m a.g.l. on temperature measured at canopy height, i.e., at 26 m a.g.l., where most direct emissions occur. The diel variation in temperature between the night and the warmest time of the day (∼ 15:00–17:00 LT) amounted to up to ∼ 8 ∘C in the wet season, 10 ∘C in the transition season, and 12 ∘C in the dry season (Fig. 5). Seasonal larger day–night temperature differences were accompanied by larger day–night OH reactivity differences (see Sect. 3.1.1). Figure 6 shows total OH reactivity as a function of temperature, which can be parameterized using an exponential function (Table 2), adapting the procedure used for the parameterization of temperature-dependent BVOC emissions in the MEGAN model (Guenther et al., 2012):
where R is total OH reactivity, T is the temperature, TS is the standard temperature (25 ∘C), RS is the total OH reactivity at standard temperature, and β is an empirical coefficient.
The dependence of OH reactivity on temperature appears to be strongest in the dry season. The parameterization for both dry seasons (Fig. 6b, d) was unified with a common exponential-fit equation as displayed in Table 2. As temperature at canopy height correlated well with OH reactivity measured at 80 m, the results discussed here indicate that plant response to environmental variables is still visible at 80 m, i.e., ∼ 50 m above the canopy top.
The seasonal differences between the temperature-related parameterization functions imply that a temperature dependence alone cannot explain OH reactivity. Additional drivers of isoprenoid emissions such as leaf phenology, biotic stress, or root inundation (potentially relevant in June 2019; see Sect. 3.1.2) may be contributing factors in seasonal differences in dependence on temperature (Alves et al., 2018; Kuhn et al., 2004b; Bracho-Nunez et al., 2012). Also, differences in turbulent transport, precipitation, and biomass burning influence the observed OH reactivity (see following sections). Nevertheless, total OH reactivity modeled from the temperature-dependent parameterization is a reasonable estimate of the measured values (Fig. S6, r2=0.61), although the deviations indicate that additional stochastic drivers may need to be considered to improve the reproduction of observed total OH reactivity.
3.3.2 Wind speed and turbulence
The wind speed observed at 26 m (inside the canopy) was on average 0.37 ± 0.33 m s−1 during the observation periods. In order to investigate the influence of wind speed on OH reactivity, data were categorized according to wind speed and day/night with high inside-canopy wind speed > 0.4 m s−1 and low inside-canopy wind speed < 0.2 m s−1. Daytime was defined as PAR > 0. Figure 7a shows that periods of high wind speed were associated with higher OH reactivity in all seasons, with more pronounced differences in the daytime. The daytime differences in median OH reactivity between periods with wind speed > 0.4 and < 0.2 m s−1 were 4.0, 7.3, 5.4, and 15.0 s−1 for March 2018, October 2018, June 2019, and September 2019, respectively. The nighttime differences were not as strong or even opposite with -1.1 to 0.7 s−1.
Several studies have shown that leaf damage through storms can lead to strong emissions of green leaf volatiles (GLVs) and terpenes (Bouvier-Brown et al., 2009; Maleknia et al., 2009; Bamberger et al., 2011; Ruuskanen et al., 2011; Kaser et al., 2013). If increased leaf damage at higher wind speeds were the cause for the differences in OH reactivity here, GLVs (Fig. 8b), i.e., indicators for leaf damage, would exhibit a strong wind-dependent pattern. This is not the case. In some observation periods, e.g., October 2018, it is even opposite (i.e., higher GLVs at low wind speed). Additionally, the effect does not appear to be prevalent at night. Therefore, we conclude that the observed correlation of higher atmospheric reactivity with higher wind speed cannot be attributed to leaf damage but to other effects. As higher wind speed correlates with higher temperature during the daytime and OH reactivity strongly correlates with temperature (Sect. 3.3.1), we cannot differentiate the causes for the observed wind–reactivity correlations with certainty. One possible wind-related effect is more efficient transport to 80 m at higher wind speeds. This means that the reactants emitted by vegetation would be transported to higher altitudes faster in such cases and consequently remain non-oxidized (and more reactive) up to higher altitudes. This effect is larger during the daytime because the abundance of highly reactive compounds in the canopy that are available for upward transport is larger and because there is stronger mixing than at night (Freire et al., 2017; Fuentes et al., 2016). It has been shown previously that conditions for vertical transport are more favorable under drier and warmer conditions, leading to larger OH reactivity observed above the canopy (Pfannerstill et al., 2018). This is supported by our data that indicate a larger difference between high- and low-wind-speed reactivity in the dry season than in the wet or transition season.
Amazonian rain events are usually due to convective storms and occur most frequently between 12:00 and 17:00 LT (Tanaka et al., 2014; Oliveira et al., 2020). The influence of rain on total OH reactivity was investigated using data from June 2019, a period with almost daily precipitation events. They were associated with sharp temperature drops due to convective cooling (Fig. 9). The time series in Fig. 9a shows an increase in hourly OH reactivity during rain events and a steep and distinct drop in OH reactivity after rain events. The composition of OH reactivity during rain events and dry periods was similar. However, the unattributed fraction was larger (39 ± 19 % vs. 23 ± 25 %) during rain events.
The increase in the hourly average during the rain events was surprising given the large contribution of OVOCs to total OH reactivity and their high water solubility. The short-term spike in observed OH reactivity during rain events can be attributed to both re-volatilization of VOCs from surfaces after wetting and the co-occurring peak in wind speed (Fig. 9), which indicates turbulent mixing, associated with the precipitation events (Sect. 3.3.2; Oliveira et al., 2020). Similarly, rapid vertical transport of particles has been observed during Amazon rain events (Wang et al., 2016).
The OH reactivity spikes were highly variable (increasing OH reactivity by 7.7 ± 6.5 s−1 or 40 ± 34 %) and coincided with peak mixing ratios of isoprene and monoterpenes (Fig. 9d), indicating wind-facilitated upward transport from the canopy to the point of observation. The large variability is due to the fact that the size of the increase in OH reactivity depends on the trace gas concentrations available for turbulent transport and therefore on the time of the day.
As an additional potential influence of rain events, there is evidence of increased BVOC emissions from wetted plant surfaces of pine trees (Kim, 2001; Janson, 1993). This may contribute to the OH reactivity spike during the rain events observed here. Soil and litter have also been shown to emit bursts of VOCs during and after rain events (Greenberg et al., 2012; Bourtsoukidis et al., 2018; Rossabi et al., 2018), attributed to both humidity-dependent microbial activity and physical desorption of compounds on the soil surfaces (the Birch effect). However, with the large distance between the point of observation and the soil in our study, we do not expect a large effect of soil emissions on the OH reactivity at 80 m a.g.l. Convective mixing during daytime storm events did not affect stable stratification in the Amazon forest canopy in a study presented by Oliveira et al. (2020). Stable thermal stratification close to the ground can stop soil emissions from reaching higher altitudes in the rainforest (Kruijt et al., 2000; Gerken et al., 2017; Santana et al., 2018; Pfannerstill et al., 2018), and it has been shown that in-canopy chemistry already strongly decreases reactant levels before they reach the canopy top (Jardine et al., 2011, 2015; Bourtsoukidis et al., 2018; Yáñez-Serrano et al., 2018). Figure 9c shows that a rain event occurring in the early morning barely increased OH reactivity, in contrast to a rain event at noon on the same day. This indicates that the reactants mainly involved in the rain reactivity peaks are subject to a diurnal cycle, as plant emissions are. Nevertheless, it cannot be ruled out that part of the additional unattributed reactivity during the precipitation events might be due to soil emissions.
The reduction in OH reactivity observed after each rain event can be explained by the co-occurring drop in temperature and irradiation, which both strongly influence plant emissions and therewith observed OH reactivity (see Sect. 3.3.1). The time lag between the temperature- and PAR-induced decrease in plant emissions and reduced OH reactivity at the tower after the rain event may be due to a time lag in plant reactions and transport times. Additionally, water soluble VOCs, especially OVOCs, can be removed from ambient air by wet deposition on the scale of the rain-affected area (Langford et al., 2010; Warneck and Williams, 2012). Figure 9e indicates such a decrease in OVOC-attributed reactivity after the rain event on the order of ∼ 30 % compared to the rain-preceding values. The vertical distribution of OVOCs before, during, and after two example rain events is shown in Fig. S7. There is no indication of re-volatilization from surfaces playing a role in OVOC OH reactivity after the rain event, as the values measured at 80 m do not surpass those at the higher altitudes except for in the turbulence-related spike during precipitation. It has to be noted that an effect of re-volatilization would be difficult to separate from influences of turbulence effects and from the recovery of photochemical processes after precipitation.
When averages of daytime periods without rain are compared to periods associated with daytime rain events, OH reactivity attributed to isoprene and monoterpenes decreased from 36 ± 19 % and 6 ± 4 % of the total, respectively, to 32 ± 18 % and 3 ± 1 %, respectively (Table S2). This can be attributed to the lower irradiation and temperature during rainy periods, which leads to lower primary BVOC emissions from plants. Additionally, terpenes can be subject to deposition on wet rainforest surfaces (Yáñez-Serrano et al., 2018). The large standard deviations reflect the high variability within rain events (Fig. 9e).
We quantified the after-rain effect on total OH reactivity values by subtracting the OH reactivity in the data point following the rain event (hourly average) from the average of the OH reactivity preceding the rain event and 2 h after. The reduction in OH reactivity after rain events was 2.5 ± 5.2 s−1 or 13 ± 23 % (average ± standard deviation) for 14 rain events in June 2019. As shown in Fig. 9b–e, the recovery to the typical diel cycle or pre-rain values after each precipitation event took up to 3–4 h for total OH reactivity, and 12 h for OVOCs, which suggests an overall negative effect of rainfall on total OH reactivity above the rainforest despite the short-term increase observed during the precipitation events.
3.3.4 Biomass burning
Air masses influenced by forest fires regularly reach the ATTO site (Pöhlker et al., 2019, 2018). Biomass-burning-influenced air masses are characterized by several markers, e.g., black carbon (Saturno et al., 2018) and benzene and acetonitrile (Yáñez-Serrano et al., 2015). Using an index derived from black carbon mass concentration and acetonitrile mixing ratios, OH reactivity observations were divided into time points strongly influenced by biomass burning and time points with low or without biomass burning influence (Sect. 2.6).
The results, displayed in Fig. 10, show that stronger biomass burning influence increases the OH reactivity observed at the ATTO tall tower. Given the fact that biomass burning releases many different trace gases (e.g., Andreae and Merlet, 2001; Koss et al., 2018), this finding is not unexpected. The difference between biomass burning and low or no biomass burning reactivity was on average 9.5 ± 2.5 s−1 (22 ± 5 %) during the daytime and 2.7 ± 0.8 s−1 (10 ± 3 %) at night. This day–night difference in the biomass burning effect on total OH reactivity may be due to (a) local anthropogenic biomass burning usually starting during the day and (b) the fact that aromatic compounds emitted by such fires have low OH reactivities, while their photooxidation products, which only can be formed during the day, have higher OH reactivities (e.g., by a factor of > 10 between benzene and its oxidation product phenol).
The effect of biomass burning on OH reactivity is smaller than the 20 %–50 % VOC mixing ratio increase due to Amazonian pasture fires reported by Christian et al. (2007), because compounds emitted by forest fires (e.g., aromatics, acetonitrile; Koss et al., 2018) are relatively unreactive towards the OH radical compared to, e.g., the terpenoids emitted by plants. For example, the reaction rate coefficient of acetonitrile is 4 orders of magnitude lower than that of isoprene. The dependence of total OH reactivity at ATTO on the activity of vegetation, characterized by isoprene abundance, is therefore stronger than its dependence on biomass burning (Fig. S8). This is also reflected in the large variability in both the biomass burning and low-biomass-burning data (Fig. 10); i.e., the categories are not particularly distinct in total OH reactivity. In contrast to Kumar et al. (2018), who found larger unattributed OH reactivity fractions in biomass burning plumes than in non-biomass-burning ambient air over the Indo-Gangetic Plain, we found no significant difference in unattributed fractions between biomass burning and no- or low-biomass-burning air at the ATTO site, because here the effect of direct biogenic emissions dominates over that of biomass burning.
The OH reactivity speciation differed between biomass burning and low- or no-biomass-burning periods. Under biomass burning influence, the share of OVOCs in total OH reactivity increased on average by 8.1 %, while the isoprenoids fraction decreased by 3.5 %. Biomass burning is a well-known source of both aromatics and nitrogen-containing VOCs (Koss et al., 2018), which, however, both have low reaction frequencies with OH. Therefore, the OH reactivity fraction of aromatics and nitrogen-containing VOCs increased by only on average 0.05 % and 0.03 %, respectively.
As the probability of drought increases in Amazonia with climate change and land use change (Swann et al., 2015; Baidya Roy, 2002; Malhi et al., 2008; Staal et al., 2020), so does the probability of forest fires (Fonseca et al., 2019). The effects observed here of biomass burning on OH lifetime and, consequently, atmospheric residence times of greenhouse gases and pollutants above the Amazon forest may therefore become larger and/or more relevant in the future.
The first measurements of total OH reactivity above the Amazon rainforest between 80 and 320 m a.g.l. were conducted during four campaigns covering three different seasons: a wet season (March 2018), a wet–dry transition season (June 2019), and two dry seasons (October 2018, September 2019). A typical BVOC-related seasonality with lower OH reactivity in the wet and transition seasons (averages of 23.7 and 19.9 s−1 in the daytime in March and June, respectively) and highest values in the dry season (averages of 29.1 and 28.2 s−1 in the daytime in September and October, respectively) was observed.
Daytime vertical gradients of the OH sink above 80 m, decreasing towards higher altitudes, were lower by about a factor of 4 than gradients between the canopy top and 80 m, indicating well-mixed conditions that allow transport of reactive VOCs from 80 m to higher levels faster than the majority of the reactants could become oxidized to less reactive species. This was visible in a vertical trend in OH reactivity composition with decreasing primary BVOCs and increasing secondary OVOCs towards higher levels. A wind speed dependency of OH reactivity measured at 80 m supports the conclusion of a strong impact of turbulent transport on the OH reactant levels observed above the canopy.
At nighttime, the vertical gradient was inversed; i.e., total OH reactivity (and even more so VOC mixing ratios) increased towards higher altitudes. This feature was attributed to deposition to the soil or canopy becoming a relevant VOC sink during the night.
The diel cycle of OH reactivity followed temperature patterns with the diel maximum around noon or in the early afternoon. Potentially due to larger day–night temperature differences, the day–night total OH reactivity difference was larger in the dry seasons (5.9–11.3 s−1) than in the wet season (3.7 s−1) or in the transition season (4.9 s−1). The lowest nighttime total OH reactivity of all observation periods was measured in September 2019, which could potentially be related to elevated ozone levels that were available for nighttime VOC oxidation.
We investigated the influence of environmental factors on OH reactivity, showing that total OH reactivity above the rainforest increased briefly during rain events due to convective transport. However, precipitation had an overall decreasing effect on total OH reactivity because of the drop in temperature and irradiation associated with these events and because of the wet deposition of OVOCs. After rain events, the OVOC-attributed OH reactivity decreased by ∼ 30 %. The OH reactivity of OVOCs was smallest in the observation period with the most rain, likely due to wet deposition.
Biomass burning increased OH reactivity by 2.7 s−1 at night and 9.5 s−1 during the day (10 %–22 %).
The temperature dependence of total OH reactivity was parameterized for dry, transition, and wet seasons. Total OH reactivity modeled from this parameterization reproduced measured values reasonably well. This parameterization could help to simplify and validate models of Amazon rainforest OH chemistry, because total OH reactivity is one holistic parameter that directly defines the OH loss frequency. Total OH reactivity could thus be used in simulations instead of many different BVOCs, where part of the OH sink is likely to be missed.
Studies of total OH reactivity in forested environments often showed significant missing, i.e., unattributed, fractions of total OH reactivity. In an attempt to close the OH reactivity budget, we applied a more comprehensive VOC detection technique than was used in previous Amazon forest studies. The OH reactivity of compounds with uncertain structure from PTR-ToF-MS measurements was calculated using averages of the reaction rate constants of all possible structures attributed to each chemical formula. These species were important OH sinks, accounting for 29 %–39 % of the seasonal total OH reactivity. Using 83 VOCs and 3 inorganic trace gases, the budget of total OH reactivity was closed within the measurement uncertainty, suggesting that previously unaccounted for OH reactivity in the rainforest was due to a combination of both primary BVOCs and oxygenated compounds. Our analysis reveals an important contribution of OVOCs to seasonal total OH reactivity of 22 %–40 %, which is a factor of > 5 more than detected in past rainforest studies and a factor of ∼ 2 more than predicted by an atmospheric chemistry model (Safieddine et al., 2017). An explanation for the large contribution of OVOCs to the OH sink is found in the meteorological conditions in the tropics with intense solar irradiation, high humidity (and therefore high OH levels), and elevated temperatures, causing fast photochemical oxidation processes. Additionally, some OVOCs can be directly emitted by plants. We also accounted for several primary BVOCs that were not included in earlier studies, e.g., green leaf volatiles, sesquiterpenes, and aromatic monoterpenes. Isoprene, generally considered the main OH sink above the tropics, contributed less than 45 % of the total OH reactivity. This shows that comprehensive measurement techniques are necessary to understand the OH sink above tropical forests and that the previously underestimated contribution of OVOCs needs to be included in models of the tropical-forest OH sink.
The data used in this study are available at https://doi.org/10.17871/atto.158.8.646 (March 2018, Pfannerstill et al., 2020a), https://doi.org/10.17871/atto.159.10.647 (October 2018, Pfannerstill et al., 2020b), https://doi.org/10.17871/atto.160.7.648 (June 2019, Pfannerstill et al., 2020c), and https://doi.org/10.17871/atto.161.14.649 (September 2019, Pfannerstill et al., 2020d).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-21-6231-2021-supplement.
EP, NR, AE, and AR conducted OH reactivity measurements. AE and AR were responsible for VOC measurements and data. EP analyzed the data and wrote the first draft of the manuscript. Ozone data and the inlet system were provided by SW, AT, and MS; methane and carbon monoxide data were provided by DW and JL; black carbon data were provided by BH, DW, FD, and CP; speciated terpene data were provided by NZ; and meteorological data were provided by MOS, AA, DW, FD, and CP. JW supervised the study. All authors contributed to manuscript writing and revision as well as read and approved the submitted version.
The authors declare that they have no conflict of interest.
This article is part of the special issue “Amazon Tall Tower Observatory (ATTO) Special Issue”. It does not belong to a conference.
The authors would like to express their gratitude to the ATTO team (particularly Reiner Ditz and Hermes Braga Xavier) for technical and logistical support and to Antonio Huxley Melo Nascimento and Thomas Klüpfel for help with the PTR-MS measurements. We thank Rodrigo Souza for providing an ozone monitor and Mohammad Kazziha for GIS plots. We are grateful for continuous support in establishing the ATTO tall tower by the Max Planck Society and the Instituto Nacional de Pesquisas da Amazônia.
This research has been supported by the German Federal Ministry of Education and Research (BMBF contracts 01LB1001A, 01LK1602A, and 01LK1602B) and the Brazilian Ministério da Ciência, Tecnologia e Inovações (MCTI/FINEP contract 01.11.01248.00). Further support was provided by the Amazonas State University (UEA), FAPESP, CNPq, FAPEAM, LBA/INPA, and SDS/CEUC/RDS Uatumã. Nora Zannoni was supported by the European Commission Horizon 2020 (grant no. FETOPEN-737071) UltraChiral project.
The article processing charges for this open-access publication were covered by the Max Planck Society.
This paper was edited by Laurens Ganzeveld and reviewed by two anonymous referees.
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