The SAMBBA field campaign was an airborne experiment carried out in the Brazilian Amazonian sector late in the dry season and during the transition from the dry to the wet season, from 14 September to 3 October 2012. Numerous atmospheric measurements were conducted on board the BAe-146 research aircraft, during 20 research flights and 67 flight hours. The BAe-146 research aircraft, from the Facility for Airborne Atmospheric Measurements (FAAM – http://www.faam.ac.uk, last access: 1 June 2018.), was based in Porto Velho – RO, but made use of other regional airports (Palmas – TO, Rio Branco – AC, and Manaus – AM airports) to extend the operational range of the aircraft (Fig. 1). During SAMBBA, the areas with positive anomalies of precipitation were mostly in western and central Amazonia, while the eastern sector was drier than the climatic average. The mean daily rainfall east of the SAMBBA flight area was typically below 1 mm. In contrast, in the western and central part, the mean daily precipitation ranged from 3 to 10 mm because of an intense cold front incursion, an early precursor of the dry-to-wet transition season. As a result, the fires in the western part of Amazonia, where most SAMBBA flights took place, were scattered and intermittent. The most intense and persistent fire activity occurred in the eastern part. The aerosol optical depth (AOD) in Porto Velho dropped from the typical 1.5 (channel 550 nm) in the first half of September 2012 to below 0.5 during SAMBBA; in contrast, the AOD was constantly above 1 in the eastern part of Amazonia.

The BAe-146 research aircraft flew with a comprehensive suite of instrumentation, measuring aerosols and cloud microphysics properties, chemical tracers, radiative fluxes, and several meteorological variables. Essential for this work were measurements of isoprene, MVK, MACR, and ISOPOOH, which were carried out using an onboard proton transfer reaction mass spectrometer (PTR-MS, Ionicon, Innsbruck, Austria) with a quadrupole detector and a typical cycle time around 3–5 s. The instrumental, operational, and calibration details are described in Murphy et al. (2010), but it is pertinent to note that (1) the quadrupole detector cannot distinguish between the isobaric molecules MVK and MACR, and its decomposition interferer ISOPOOH, so it reports the data at m/z 71 as the sum of three isomers, even though it was only calibrated for MVK + MACR (Liu et al., 2016); (2) the conversion yields of ISOPOOH into MVK and MACR was observed to be greater than 70 %, but the decomposition is known to be highly sensitive to instrumental settings such as temperature, contact time, and type of surface materials, especially transition metal surfaces (Liu et al., 2013; Nguyen et al., 2014; Rivera-Rios et al., 2014, Liu et al., 2016, Bernhammer et al., 2017); and (3) there is a well-known interference in the isoprene signal at m/z 69 in biomass burning plumes from furan. The PTR-MS was calibrated post-flight using a calibrated gas standard provided by Apel Riemer Environmental Inc. We compared the PTR-MS isoprene data with the isoprene data derived from the whole air sampling (WAS) system on the aircraft to correct the PTR-MS isoprene data due to a probable interference from furan at m/z 69 in biomass burning plumes. The WAS system was described in Hopkins et al. (2011) and consists of discrete air samples collected in 3-liter silco-treated stainless steel canisters with subsequent post-flight analysis by GC-FID. In the background environment, the agreement between the two systems was excellent (isoprenewas / isopreneptrms=  0.81, SD = 0.56), while in biomass burning regions we estimated a high furan contribution in fresh (isoprenewas / isopreneptrms=  0.25, SD = 0.12) and aged (isoprenewas / isopreneptrms=  0.77, SD = 0.57) smoke plumes. The isoprene data have been adjusted accordingly.

In addition, NO measurements were conducted using a chemiluminescence instrument (Air Quality Design Inc., Wheat Ridge, CO, USA), with the NO2 measured using a second channel after photolytic conversion to NO. The photolytic conversion eliminates the possible interference from NOz on the NO2 channel. The detection limits were close to 10 pptv for NO and 15 pptv for NO2 for 10 s averaged data, with estimated accuracies of 15 % for NO at 0.1 ppbv and 20 % for NO2 at 0.1 ppbv (Allan et al., 2014). For the O3 and CO analyses, we used the TEi49C and AL5002 VUV fast fluorescence onboard instruments, respectively (Gerbig et al., 1996, 1999; Palmer et al., 2013). Calibration gases were supplied to the rack from the gas bottle stowage, and the air sampling from the atmosphere was via the air sample pipes and a dedicated window-mounted inlet system.

During the planning phase, SAMBBA flights were classified according to their scientific objectives as either biogenic or biomass burning flights (Fig. 1). For this study, we selected 13 flights according to the gaseous chemistry data available (Table 1). Additionally, we only considered the data collected below 2000 m and between 11:00 and 18:00 LT (local time) to capture the difference in the oxidative capacity along the altitude during daytime, since the OH concentration is regulated by photochemistry (Elshorbany et al., 2009). Despite the classification in the planning phase, parts of some flight tracks passed through unpolluted regions, smoke haze, or even interception of fresh smoke plumes. To maximize the use of data, we classified parts of the flight tracks according to the CO mixing ratio values as background (BG) and biomass burning. According to Andreae et al. (2012) and several references therein, the Amazon rainforest atmosphere has a background CO mixing ratio typically around 100 ppbv. However, the mean CO inflow into the Amazon Basin during the SAMBBA period at 500 hPa, retrieved from Atmospheric Infrared Sounder (AIRS) measurements on board the AQUA satellite, ranged between 140 and 160 ppbv (Fig. 2 and Supplement Fig. S7). This hemispheric inflow is homogeneous along the vertical column up to around 400 hPa. In fact, there were only few SAMBBA samples with CO mixing ratio values below 100 ppbv. Therefore, we adopted a threshold of 150 ppbv to represent the background of CO in the Amazon atmosphere during the SAMBBA campaign.

As O3 is formed photochemically downwind during smoke aging, the enhancement ratio of O3 to CO is acceptable as a reliable indicator of the smoke plume age (Andreae et al., 1994; Parrish et al., 1993). Furthermore, due to the lack of NOy / NOx ratio in SAMBBA, we used the ratio of O3 to CO as a proxy for smoke plume age. The biomass burning flight tracks with [CO] > 150 ppbv were then reclassified as fresh smoke plume (FP) or as aged smoke plume (AP) interceptions according to the following. ERΔO3/ΔCO=O3smoke-O3backgroundCOsmoke-CObackground During the BG flight tracks (CO ≤ 150 ppbv), the mean value of the O3 mixing ratios near the surface (< 500 m) was 21 ± 7 ppbv, which we then adopted as the O3 mixing ratio background. In Table 2, we list the values of ER[ΔO3]/[ΔCO] and the estimated smoke plume age for several smoke measurements in Amazonia and Africa. Jost et al. (2003) found the value of ER[ΔO3]/[ΔCO]= 0.1, 2 h after emission in Otavi, northern Namibia; and Andreae et al. (1988) found 0.08 for fresh biomass burning (650 m altitude) in the Amazon Basin region. Comparable values of ER[ΔO3]/[ΔCO] (0.09) were observed in other young smoke plumes with 0.5–1.0 h aged during the Southern African Regional Science Initiative 2000 – SAFARI 2000 (Hobbs et al., 2003; Yokelson et al., 2003). Mauzerall et al. (1998) reported 0.15 for FPs with fewer than 4.8 h over regions with active fires in the northeast region of Brazil and in Africa. In short, we classified the parts of the flight tracks as background (BG) when [CO] ≤ 150 ppbv, and the biomass burning flights ([CO] > 150 ppbv) into two subgroups of FP, with [O3] / [CO] < 0.1 and AP, with [O3] / [CO] ≥ 0.1.

The OH concentrations from the [MVK + MACR + ISOPOOH] / [isoprene] ratio using the sequential reaction model were originally developed by Apel (2002) and Stroud et al. (2001) and modified according to the approach of Karl et al. (2007). This method can be used to investigate the impact of vertical transport, representing the processing time of the isoprene and its oxidation products from the surface to the atmosphere through the ratio of PBL depth and the convective velocity scale. To have a more accurate OH estimation, we modified the processing time t to represent not only the vertical transport but also the horizontal atmospheric circulation, where t was calculated as a function of the enhancement ratio ER[ΔO3]/[ΔCO] (see Supplement Fig. S5). Table 2 shows the plume age time and the enhancement ratio ER[ΔO3]/[ΔCO] values used in the new approach. This method is based on observations that the isoprene reaction rate with OH (rate coefficient ≅ 1.0 × 10-10, lifetime ≅ 1.4 h) is more important than with O3 (rate coefficient ≅ 1.3 × 10-17, lifetime ≅ 1.3 day) during the daytime and assuming a constant reaction rate. Following the simplified sequential reaction model, we can estimate OH concentration, in molecules cm-3, with the following analytical expression: [OH]=ln⁡1+MVK+MACR+ISOPOOHisoprene⋅(Kiso-Kprod)Kiso⋅0.55((Kiso-Kprod)⋅t), where kiso and kprod are, respectively, the reaction rate constants of isoprene + OH (1.1 × 10-10 cm3 molecules-1 s-1), and [MVK + MACR + ISOPOOH] + OH (6.1 × 10-11 cm3 molecules-1 s-1), and we are assuming a total yield of 0.55 of MVK + MACR + ISOPOOH from the OH + isoprene reaction (Apel, 2002; Karl et al., 2007). We estimated the processing time as t=5.3×105.4⋅ER[ΔO3]/[ΔCO] (seconds), which is the fitting function of several previous measurements of ER[ΔO3]/[ΔCO] (Supplement Fig. S3) and plume age observations in tropical and subtropical sites (Table 2).

Figure 3 depicts CO, NOx, and O3 mixing ratios measured at different altitudes, up to 2 km, and time of the day, between 11:00 and 18:00 LT. In Fig. 3, the flight tracks are separated according to the BG, FP, and AP classification, while Table 3 shows typical values of CO, NOx, and O3 mixing ratios measured in this study and during several previous airborne campaigns in Amazonia and savannah areas in Brazil. During the SAMBBA field experiment, in BG conditions (i.e., CO < 150 ppbv), the NOx mixing ratio ranged from 50 to 200 pptv. Torres and Buchan (1988) reported measurements of NO mixing ratios ranging between 20 and 35 pptv during the Amazon Boundary Layer Experiment (ABLE-2A) between July and August 1985. Modeling results of Jacob and Wofsy (1988) found NOx mixing ratio values around 200 pptv, with the NO mixing ratio values similar to the ABLE-2A observations that were conducted over the Amazon rainforest. Also in the Brazilian Amazon Basin during the wet season, aircraft measurements as part of the NASA Amazon Boundary Layer Experiment (ABLE-2B), showed NOx mixing ratios ranging from 4–68 pptv (Singh, 1990). Comparing our results with these previous studies, the SAMBBA experiment showed a slight influence from polluted regions. More recently, Liu et al. (2016) used four sets of different MCMs and estimated that NO mixing ratio using the NO vs. HO2 isoprene chemistry (fHO2 : fNO ∼ 0.6–1.4) would be around 20–40 pptv of NO based on measurements in the Amazon, lower than that obtained in our study. On the other hand, flight tracks in biomass burning areas showed high values of NOx in FP (50–1250 pptv) and AP (50–950 pptv) compared with other studies in forest areas of Amazonia, including a study in the cerrado area in Brazil (∼ 750 pptv) conducted by Crutzen et al. (1985) during the dry season.

The O3 mixing ratios in the BG environment reached 40 ppbv at about 600 m altitude during flight B735 (at 11:30 LT, Fig. 3), although typical values ranged from 10 to 45 ppbv (< 2000 m; Table 3). This value of 40 ppbv at 600 m altitude is nearly 2 times the mean value of the O3 mixing ratio that we used as background in the enhancement ratio, and even out of the range of the standard deviation (21 ppbv, SD = 7). As a secondary pollutant, O3 is commonly found in low concentrations near the surface, a fact not observed in our study even for the BG samples. Bela et al. (2015) reported O3 ranging from 10 to 20 ppbv during the wet-to-dry transition season (May–June 2009), measurements performed in a clean atmosphere during the Regional Carbon Balance in Amazonia (BARCA-B) campaign. In contrast, during the BARCA-A campaign in November–December 2008 (during the dry-to-wet transition season), the O3 mixing ratio ranged from 40 to 60 ppbv in an area influenced by fires, values which are comparable with FP (10–75 ppbv) and AP (20–70 ppbv), and even in BG conditions (10–45 ppbv) during SAMBBA.

In terms of CO and NOx, flight tracks classified as FP were the most polluted of the campaign. The CO and NOx mixing ratios for FP reached, respectively, values above 3000 and 60 ppbv at 600 m from the surface between 11:00 and 12:00 LT. The enhancement of CO and NOx mixing ratios near the surface suggests significant vertical transport due to the hot plume buoyancy, which may increase the tracer lifetime released to the atmosphere. The vertical transport can be observed mainly for CO at different altitudes and time of day, since the CO is preserved longer along the plume when compared with NOx. The measurements in fresh biomass burning plumes also capture higher levels of CO mixing ratios (≅ 500 ppbv) at 1.4 and 2 km of altitude. Yokelson et al. (2007), during the Tropical Forest and Fire Emissions Experiment (TROFFEE), reported a vertical transport mechanism called a “mega-plume” at 2 km altitude during a flight south of the Amazon rainforest (from Manaus to Cuiabá), with the CO mixing ratio reaching 1200 ppbv. The TROFFEE experiment used airborne measurements during the 2004 Amazon dry season, and reported, on 8 September, the presence of a massive plume formed by numerous fires. During SAMBBA campaign, we also detected the presence of similar plumes during flight B742, classified mostly as FP, with a unique CO mixing ratio value, peaking at ∼ 5000 ppbv at about 600 m. These results demonstrate the strength of vertical transport during a fresh biomass burning event, with the plume injection height up to 2 km. Freitas et al. (2006, 2007, 2010) highlighted the importance of representing the injection height of biomass burning plumes in numerical models to describe the regional smoke distribution. Trentmann and Andreae (2003) also demonstrated a large impact of fire emissions on the chemical composition in a young biomass burning plume using a 3-D chemical transport model and direct observations. These authors reported simulated high values near the fire (z ≅ 150 m) for CO and NOx, with mean values around 18 000 ppbv and 404 ppbv, respectively. On the other hand, Andreae et al. (2012) reported CO mixing ratios up to 400 ppbv in a smoky region in the southern Amazon Basin during the BARCA-A experiment. The highest values were found at about 1000 m altitude, late in the dry season (November 2008). In this study, the CO mixing ratio measurements in FP and AP ranged from 150 to 900 ppbv and from 150 to 450 ppbv, respectively. The CO mixing ratios in FP (150–900 ppbv) are comparable with values found by Reid et al. (1998) in a cerrado area (440–763 ppbv) and some forest studies (up to 600 ppbv) conducted by Andreae et al. (1988), Kaufman et al. (1992), and Yokelson et al. (2007). The values found in AP agreed with values of CO mixing ratios from forest areas, impacted by smoke haze plumes (Table 3).

In Fig. 3, during most of the flight tracks classified as AP, the NOx mixing ratio values were below 2 ppbv, except for a peak of 6 ppbv at 600 m from the surface between 11:30 and 12:00 LT, a value below that observed in the FP environment (60 ppbv). Conversely, the O3 mixing ratio results in FP presented high levels (≅ 80 ppbv) around 12:10 LT at 1300 m altitude. We also investigated the high levels of CO and NOx mixing ratios found in FP corresponding to the same flight in which we also detected high levels of O3 in AP. In fact, Fig. 4 shows the track of flight B742 in the transition from a remote site impacted by FP to an urban site impacted by AP in Palmas – TO (O3 ≅ 80 ppbv). The mean value of O3 found in FP was 31 ppbv (SD =  14), which is 29 % lower than measured for AP (44 ppbv, SD =  13 ppbv), since O3 is produced as a secondary product from the interaction between VOCs and NOx. The O3 mixing ratios in FP peak at about 60 ppbv near the surface (200–600 m) and, for most cases, plumes with about 40 ppbv were observed both near the surface and in high altitudes (Fig. 3). During the TROFFEE experiment, Yokelson et al. (2007) found O3 mixing ratios of about 30 ppbv in smoke haze layers in Amazonia. Our results showed higher values for O3 mixing ratios, ranging from 10 to 75 ppbv in FP and 20 to 70 ppbv in AP. Agreeing with SAMBBA results, Reid et al. (1998) found O3 mixing ratios ranging from 60 to 100 ppbv during the SCAR-B experiment in the 1995 dry season, and Kaufman et al. (1992) found similar levels of O3 in a forest site in Amazonia during BASE A (Table 3).

Information about isoprene transport and chemistry can be derived from the isoprene abundance in the atmosphere and the ratio of its oxidation products over isoprene, [MVK + MACR + ISOPOOH] / [isoprene]. During the day, the isoprene chemistry is mainly affected by the distance from the emission source (transport time), photochemical degradation, and availability of OH, which react with isoprene to produce (among other chemical species) MVK, MACR, and ISOPOOH (Kuhn et al., 2007; Liu et al., 2016). During SAMBBA, the mean isoprene mixing ratio in BG was 2.8 ppbv and 1.5 ppbv for the boundary layer and cloud layer, respectively. We also detected higher values of O3 (40 ppbv at 600 m) in BG, shown in Fig. 3, coinciding with the interpolated cross section of isoprene (≤ 4 ppbv at 600 m), also in the BG environment (Fig. 5). As mentioned by Barket et al. (2004), a sequence of reactions initialized by the reaction of isoprene with OH leads to the production of organic peroxy radicals (RO2), which then react with NOx promoting the O3 formation observed during the BG flights tracks. Table 4 summarizes the mean values of isoprene and the oxidation ratio [MVK + MACR + ISOPOOH] / [isoprene] during SAMBBA, and previously reported airborne measurements in remote areas and biomass burning environments. The isoprene mixing ratios measured during SAMBBA in the BG environment agree with values reported in pristine areas of the Amazon forest (Greenberg et al., 2004; Greenberg and Zimmerman, 1984; Gregory et al., 1986; Helmig et al., 1998; Kuhn et al., 2007; Lelieveld et al., 2008; Rasmussen and Khalil, 1988; Zimmerman et al., 1988). Some studies conducted in the Amazonian tropical forest (e.g., Greenberg et al., 2004 and Kuhn et al., 2007) reported isoprene mixing ratios up to ∼ 7 ppbv, values higher than we found during the SAMBBA campaign.

On average, we found a reduction of isoprene in FP (1.4 ppbv), and a more discrete reduction in AP (2.4 ppbv), relative to the BG value (2.8 ppbv), within the PBL (< 1200 m), producing a lower value around 50 % and 14 %, respectively. In contrast, we observed above the PBL (> 1200 m) an impressive increase of about 60 % of the isoprene in AP (2.4 ppbv) relative to the BG value (1.5 ppbv), which is about the same mean value found in FP (1.6 ppbv). These high levels of isoprene at higher altitudes in air masses affected by biomass burning emissions are likely to be associated with the heat released from vegetation fires affecting nearby plants with enough energy to release significant amounts of isoprene to the atmosphere, especially in tropical forest fires in Brazil (Ciccioli et al., 2014). Müller et al. (2016), for example, found isoprene mixing ratios up to 15 ppbv in a smoke plume from a small forest fire in Georgia, USA. We also found higher isoprene mixing ratios in the upper levels (> 1200 m) of smoke areas when compared with pristine mixed layer studies mentioned previously. These results reinforce the hypothesis that fire activity promoted the isoprene transport to higher altitudes both in fresh (≅ 6 ppbv, 1700–2000 m) and aged plumes (≅ 4 ppbv, 1600–2000 m) during SAMBBA flights (Fig. 5). In Fig. 6, we also verified the average isoprene mixing ratio (< 2000 m) in AP (2.4 ppbv) was 71 % higher than FP (1.4 ppbv) and similar to the mean value measured in BG (2.6 ppbv).

In smoke plumes, biomass burning tracers, such as acetonitrile and acetaldehyde, are present at high concentration, while the [MVK + MACR + ISOPOOH] / [isoprene] ratio is low. In contrast, as an aging effect, smoke plumes typically have higher values for the [MVK + MACR + ISOPOOH] / [isoprene] ratio, since there is more time for the isoprene degradation. According to Apel et al. (2002), the high value for kOH is responsible for the majority of the chemical processing of isoprene by OH. As the rate constant of OH with MVK and MACR are lower than isoprene-OH, we expect an increase in the ratio [MVK + MACR + ISOPOOH] / [isoprene], especially in a polluted environment in the boundary layer. Figure 7 presents the plume interception during the flight B732, between 10:00 and 11:30 LT, in which it is possible to observe the different altitude interceptions through the biomass burning tracers and [MVK + MACR + ISOPOOH] / [isoprene] ratio. In this study, we found the [MVK + MACR + ISOPOOH] / [isoprene] ratio mean value ranging from around 1.7 in the boundary layer up to 3.3 in the cloud layer for BG conditions, with AP presenting a similar value (2.3) for both boundary layer and cloud layer. In contrast, FP had the highest value in the boundary layer (7.0) and cloud layer (6.1), values reported by Kuhn et al. (2007), in the tropical forest in Brazil (north of Manaus).

We did not find any substantial variation above the PBL in [MVK + MACR + ISOPOOH] / [isoprene] ratio associated with the presence of smoke in AP (2.8) but did find an increase in the BG value (3.3) in the upper levels (> 1200 m). The FP is more active within the boundary layer than in upper levels, with the isoprene oxidation ratio about 6.1 above 1200 m. Comparable with our results in FP, Kuhn et al. (2007) during the Cooperative LBA Airborne Regional Experiment (LBA-CLAIRE-2001), also found [MVK + MACR + ISOPOOH] / [isoprene] ratio values up to 2, below 1000 m of altitude, and between 2 and 10, within the 1000–2000 m vertical layer. In summary, we found a strong increase in the isoprene oxidation ratio from the surface up to 2000 m for FP relative to the BG and AP observed during SAMBBA and other previous studies in biomass burning environments (Table 4). The energetic process that occurs during the biomass burning causes the isoprene plume to be transported rapidly to higher levels, impacting the isoprene oxidation level, with FP samples presenting a higher [MVK + MACR + ISOPOOH] / [isoprene] ratio.

We also observed during SAMBBA campaign values of the [MVK + MACR + ISOPOOH] / [isoprene] ratio above 6 in BG air masses above 1800 m and between 12:00 and 13:30 LT. In contrast, in FP and AP, values in the range 4–6 are equally distributed in the vertical profile, with some high values near the surface (Fig. 5). Along the cloud layer (1200–2000 m), we found that isoprene oxidation in BG environment increase (94 %) as in FP levels (Table 4). Karl et al. (2007) also reported evidence of an increase in the oxidizing power of the atmosphere in the transition from PBL to cloud layer (1200–1900 m) during the TROFFEE experiment, with the [MVK + MACR + ISOPOOH] / [isoprene] ratio ranging from 0.39 up to 1.2 between 300 and 1800 m, already into the cloud layer (CL). Although lower values for the [MVK + MACR + ISOPOOH] / [isoprene] ratio were found during TROFFEE compared with LBA-CLAIRE, both studies have suggested the occurrence of an oxidizing power in the transition from the PBL to the CL. In both cases, there was a positive gradient, increasing the [MVK + MACR + ISOPOOH] / [isoprene] ratio. Furthermore, Helmig et al. (1998) reported similar behavior in a remote Peruvian Amazonia site, with the [MVK] / [isoprene] ratio equal to 0.15, 0.19, and 0.48, near the surface (≅ 2 m), in the PBL (91–1167 m), and above the PBL (1481–1554 m), respectively. The [MVK + MACR + ISOPOOH] / [isoprene] ratio increasing toward the top of the PBL and CL is likely to be due to the enhancement of the photolysis rates. Direct experimental data reported by Mauldin et al. (1997) also indicated significant changes above and inside cloud decks due to cloud edge effects on photolysis rates that have a major impact on OH production rates. Figure 8 presents the density distribution for the [MVK + MACR + ISOPOOH] / [isoprene] ratio along several altitude layers during SAMBBA. In FP, the average [MVK + MACR + ISOPOOH] / [isoprene] ratio was 6.3 at 500–1000 m, 7.6 at 1000–1500 m, and returning to 5.9 at 1500–2000 m. These results are consistent with the increase in the oxidative capacity in the transition from the PBL to the CL, reported by Mauldin et al. (1997) and Karl et al. (2007), with SAMBBA measurements showing an average [MVK + MACR + ISOPOOH] / [isoprene] ratio constantly increasing in BG and the highest value at 500–1000 m in AP. The results show that the isoprene oxidation reaction is also enhanced at higher altitudes in the BG environment, increasing from 1.4 at the first 500 m to 3.4 at 2000 m. Another characteristic observed during biomass burning events is their capacity to disturb the isoprene oxidation reactions, especially in the fresh plumes. As showed in Fig. 8, the isoprene oxidation is higher in FPs at lower altitudes (∼ 500) than in aged smoke, anticipating near the surface a complex chain of oxidation reactions which may be related to SOA formation. Rohrer et al. (2014) compared observations of OH radicals in different environments characterized by high VOC concentrations; they found that VOC degradation not only accelerates but also occurs at the maximum rate if NOx is present in adequate amounts. Thus, biomass burning is a source of NOx, favoring an increase in the oxidative capacity. According to Rohrer et al. (2014), the OH recycling mechanism is shown to be active not only in pristine biogenic air masses but also in the interface region between anthropogenic and biogenic emissions, such as in the region surrounding Manaus – AM, where urban and biogenic emissions are mixed.

The abundance of OH in the atmosphere is determined by equating the kinetic rate of its production and loss. Due to the absence of OH measurements during SAMBBA, we inferred the OH concentrations using a sequential reaction model to the observed profiles of the [MVK + MACR + ISOPOOH] / [isoprene] ratio. Table 4 presents the average values of OH concentration in remote areas and biomass burning environments worldwide, and the estimated OH concentration calculated via the sequential reaction model approaches from Karl et al. (2007) and via the approach proposed in this study. In FP, the estimated OH concentration reached the highest value within the PBL (1.4 × 106 molecules cm-3), when compared with AP or even with the BG environment, both with OH concentration ∼ 0.1 × 106 molecules cm-3. The photochemical environment in young biomass burning plumes differs from the clean conditions, especially near the surface. Hobbs et al. (2003) found OH concentrations of about 1 × 107 molecules cm-3 for a fresh plume from savanna fire in South Africa, values higher than those found in our estimation. In the CL, the estimated OH in AP showed a reduction of 15 % relative to BG (0.5 × 106 molecules cm-3) environment, in opposition to increased pattern in FP (1.2 × 106 molecules cm-3). The estimated OH concentration corroborates the hypothesis that the biomass burning event can intensify the oxidative capacity at low altitudes.

Figure 9 shows the vertical profile of estimated OH concentration in different chemical regimes, comparing the sequential reaction model according to the original approach of Karl et al. (2007) with the new approach used in this work. Throughout the altitude range 0–2000 m, the difference in OH calculation between the two methods was approximately 2 orders of magnitude, although presented a similar pattern in the different chemical regimes. Flight tracks classified as BG tend to increase the OH concentration along the altitude, with the inflection point occurring before the 1000 m. Differing from BG environments, FP presents a decreasing pattern for OH concentration after 1000 m of altitude, with the AP in an intermediate state. Our results suggest that in the FPs, the vertical transport predominates with the oxidative capacity reaching its maximum at 1000 m. In the flight tracks classified as BG, we observed the widest variation in the average OH concentration using the new sequential reaction model (Fig. 9, on bottom), especially in upper levels (0.5–1 × 106 molecules cm-3), although reported a lower confidence level in this region due to a reduced number of samples. In all three different chemical regimes, the vertical profile of OH concentration presented an increase near to CL (∼ 1000 m), in agreement with previous studies (Karl et al., 2007; Kuhn et al., 2007; Langford et al., 2005; Mauldin et al., 1997).

Similar to the OH vertical profile, the amount of NOx increases in the boundary-cloud layer (500–1000 m) for FP and AP, with the O3 pattern presenting ∼ 20 ppbv higher than the values from BG environment. In contrast, the highest values for OH in BG environment was found close to 2000 m of altitude, which reinforce the Lelieveld hypotheses (Lelieveld et al., 2008) of the reaction of isoprene-derived peroxy radicals with organic peroxy radicals as an alternative pathway to OH production in an unpolluted environment.

The estimated OH concentration values presented in this study agree in order of magnitude with most modeled and observed values previously reported for Amazonia and other forest areas. Prediction studies in a forest site at Surinam, conducted by Warneke et al. (2001), estimated a concentration of OH ranging from 1 to 3 × 105 molecules cm-3 (24 h average), and Williams et al. (2001) calculated a range of 0.6–1.1 × 106 molecules cm-3 during daytime. During the Guyanas Atmosphere–Biosphere exchange and Radicals Intensive Experiment with a Learjet (GABRIEL) experiment in  October 2005, the observed average OH concentration in the boundary layer (< 1 km) over the Suriname rainforest in the afternoon was 4.4 × 106 molecules cm-3 (Kubistin et al., 2010). On the other hand, Dreyfus et al. (2002) reported high levels of OH concentration (8–13 × 106 molecules cm-3) in the boundary layer over a forest area in Sierra Nevada, California; this forest site was influenced by wind flow patterns, transporting anthropogenic volatile organic compounds and NOx from the Sacramento region toward the Sierra Nevada.

Several studies investigated the uncertainties in the isoprene oxidation mechanism, and most of them focus on OH concentration levels through observational and modeling studies (de Gouw et al., 2006; Kubistin et al., 2010; Kuhn et al., 2007; Lelieveld et al., 2008; Lu et al., 2012; Whalley et al., 2012; Yokelson et al., 2007). Under a high isoprene and low NO atmospheric regime, there is a controversial discussion about the impact on the oxidative capacity in forest sites. Some observations indicate that high OH levels cannot be accounted for by the conventional OH production and recycling mechanisms (Rohrer et al., 2014), but some suggested that the enhanced OH signal is caused by instrumental artifacts rather than the ambient OH (Mao et al., 2012). Our calculated OH with the observational constraints is consistent with previous empirical estimates by Warneke et al. (2001) that estimated OH concentration around 1–3 × 105 molecules cm-3 (24 h average); Williams et al. (2001) also found 0.6–1.1 × 106 molecules cm-3 during daytime without augmented OH recycling mechanisms developed to account for the recent higher than expected OH observations. According to the most recent results in the Amazon rainforest (Liu et al., 2016), the order of magnitude of the OH concentration estimated in our study agrees well with both OH concentrations close to 1 × 106 molecules cm-3.