All data presented were collected at the T3 site (3.2133∘ S, 60.5987∘ W), located 70 km west of Manaus, Brazil, during the GoAmazon2014/5 campaign (Martin et al., 2016). The T3 site is located within pasture land located 10 km northeast of Manacapuru, Brazil. The site included the Atmospheric Radiation Measurement (ARM) Mobile Facility no. 1 (AMF-1), the ARM Mobile Aerosol Observing System (MAOS), and four modified shipping container laboratories containing instruments deployed by universities and other research organizations.

Ambient ultrafine-particle composition was characterized using TDCIMS. TDCIMS is an instrument designed specifically for the measurement of the molecular composition of size-resolved ultrafine aerosol particles (Smith et al., 2004; Voisin et al., 2003). In brief, sampled atmospheric particles are charged by a unipolar charger and are collected via electrostatic deposition on a platinum (Pt) filament over varying collection times. During this campaign, collection times were either for 1 h or 30 min, depending on the anticipated sample mass. A typical sample mass collected on the filament ranged from 10 to 100 ng. After collection, the filament was moved into an atmospheric pressure chemical ionization source region and resistively heated to desorb the particulate-phase components. These desorbed components were chemically ionized and detected using a quadrupole mass spectrometer (Extrel Corp.). A zero-air generator (Parker Hannifin, model HPZA-3500) provided the source of reagent ions (H2O)nH+ and (H2O)nO2- (n=1–3); TDCIMS operation with these ion chemistries is referred to as either the positive- or negative-ion mode, respectively. Complete mass spectra of desorbed compounds were obtained at the beginning of IOP1 (Fig. S1 in the Supplement) to determine ions with the highest ion abundances. These ions were then measured for the duration of the campaign by operating the quadrupole mass spectrometer in “selected-ion mode”, in which the quadrupole mass spectrometer rapidly switched among approximately 12 ions to optimize sensitivity with high temporal resolution.

Both positive- and negative-ion-mode chemical analyses were performed during the two IOPs and are publicly available on the campaign data archive (Smith, 2016). During IOP1, several days of measurements were impacted by intermittent power outages and brownouts. IOP2 was characterized by comparatively lower concentrations of ultrafine particles, which is consistent with prior observations (Martin et al., 2010; Varanda Rizzo et al., 2018). Because of this, we focus our analysis on 10 consecutive days during IOP1 when instruments were operating consistently. This period also happened to coincide with the arrival of two distinct and consecutive air masses, which allows for more accurate side-by-side comparison of aerosol properties during these periods.

Ambient particles were sampled through 3 m of Cu tubing with a 0.63 cm inside diameter. The inlet extended 0.5 m above the roof of the laboratory and was curved downward and covered with a screen to prevent rain and insects from entering. Ambient particles during GoAmazon2014/5 were not size-selected prior to collection on the filament because of low ambient concentrations. The collection process, however, is inherently dependent on particle mobility (McMurry et al., 2009). In order to determine the size-dependent collection efficiency, tests were run at the start of the campaign by generating and collecting ammonium sulfate particles in the diameter range of 8–90 nm. The size-dependent TDCIMS sampling collection efficiencies were used to determine the volume mean diameter and estimated mass of each sample, as described in Smith et al. (2004).

To complement the TDCIMS dataset, high-resolution time-of-flight aerosol mass spectrometry (AMS; Aerodyne, Inc.) was used to characterize non-refractory compounds in PM1 at the T3 site (ARM, 2018a; de Sá et al., 2018). A seven-wavelength aethalometer was located at MAOS and measured black-carbon mass concentration (ARM, 2018b). The planetary boundary layer height (ARM, 2018c), determined using the Heffter number method (Heffter, 1980), was measured at MAOS. A scanning mobility particle sizer (ARM, 2018d) determined the number-size distributions spanning the mobility diameter range of 10–460 nm. Wind direction, wind speed, relative humidity, temperature and rainfall were measured at AMF-1 (ARM, 2018e). Six hour back-trajectory frequency simulations were determined for the time period of interest using the NOAA HYSPLIT transport model, which uses the GDAS 1∘ meteorology (Rolph et al., 2017; Stein et al., 2015).

PCA was performed using the “princomp” function of the R statistical software package (R, 2011). A hierarchical cluster analysis was performed using Ward's averaging method in the “hclust” function in R. Ward's minimum variance method of hierarchical clustering was used, which groups species within the same cluster to minimize the total variance (Wilks, 2011). The purpose of this analysis is to identify species or groups of species that may have unique sources, trajectories or other physicochemical characteristics. Cluster analysis was done for the following TDCIMS negative- and positive-ion-mode species: C2H4N- (m/z 42), C2H3O2- (m/z 59), HSO4- (m/z 97), Cl- (isotopes m/z 35 and 37), HC2O4- (m/z 89), NH4+(H2O) (m/z 36), K+ (m/z 39 and 41), C3H10N+ (m/z 60), C5H7O+ (m/z 83), C5H8NO+ (m/z 98) and C7H9O2+ (m/z 125). Cluster analysis was also done for the following AMS species: organic, ammonium, nitrate, sulfate and chloride. A separate cluster analysis was performed for quality assurance and demonstrated that the three clusters presented in Sect. 3.3 are statistically significant and different from one another.

The 10 consecutive days that are the focus of this study can be characterized by two distinct air mass types, as determined from meteorological data and AMS-derived positive matrix factorization (PMF) factors (de Sá et al., 2018). The first period, referred to as the anthropogenic period, was from 14 March to mid-morning on 19 March, and the second period, the background period, was from mid-morning on 19 March to 24 March. The AMS-derived biomass-burning factor (BBOA), associated with levoglucosan, and the anthropogenically dominated factor (ADOA), associated with mass fragment 91 or “91fac” (C7H7+), were as much as 3 times larger during the anthropogenic period than background period (de Sá et al., 2018). Anthropogenic influence during this campaign, as determined using ADOA, most strongly resembled cooking emissions. Correlations between ADOA; cooking emissions; aromatics like benzene, toluene and xylene; and increased particle counts verify the link to anthropogenic influence from Manaus (de Sá et al., 2018). The particle number-size distribution, shown in Fig. 1, for the anthropogenic period saw higher number concentrations of particles over the diameter range of 10–100 nm (N100). Particle size distributions for the background period were comparable to previous measurements in the Amazon Basin, featuring a bimodal distribution with peaks at roughly 50 and 150 nm and peak concentrations of approximately 103 particles cm-3 (Fig. S2; Artaxo et al., 2013; Gunthe et al., 2009; Pöhlker et al., 2016; Varanda Rizzo et al., 2018). The average total mass concentration as determined by AMS for the anthropogenic period was 2.5±0.9 µg m-3. The T3 site experienced approximately 4 h of rain on 19 March, ending at about noon UTC (all times are presented as UTC time, which is 4 h ahead of local time), and the first and only new particle formation event of this 10 d period was observed. After this event on 19 March, number concentrations of particles were, on average, much lower than the prior period. The average total mass concentration for the background period was determined to be 1.2±0.8 µg m-3. A similar trend in total mass concentration between background and polluted conditions was observed during the Southern Oxidant and Aerosol Study (SOAS), where larger particle mass concentrations were observed during times with polluted air mass influence and, when followed by a period of rainfall, smaller mass concentrations were observed (Liu and Russell, 2017). Occasional rainfall was seen during the background period, resulting in wet deposition of aerosol particles. Additionally, a back-trajectory analysis, presented next, provides a more likely reason for these two distinct periods.

Wind direction data shown in Fig. 1, as well as NOAA HYSPLIT data shown in Fig. 2, suggest a reason for the two distinct periods. Back trajectories show that air masses during the anthropogenic period either pass through Manaus or south of Manaus prior to arrival at the T3 site. During this period, air masses most frequently passed over the main roadway that connects Manaus with Manacapuru, a neighboring city with a population of 93 000. Along this roadside are homes, agriculture and brick kilns, all of which contribute to local gas and particle emissions. In contrast, during the background period, air masses arrived at the T3 site most frequently from the northeast and west. Air masses that were measured at the site typically originated from densely forested regions northeast to west of Manaus. Less frequent were periods where air masses reaching the site originated from the east and were influenced by the Manaus metropolitan area. For example, during the evening of 21 March there was a period of increased number concentration, and as winds were quite stagnant at night, it is possible that a local emission source could have impacted the site during that period. Wind direction on this day corresponded with air masses arriving to the T3 site from the Manaus area.

Estimated masses of ultrafine particles sampled by TDCIMS were determined and compared for the two periods (Fig. S3). During the anthropogenic period there was no distinct diurnal pattern observed, with an average of ∼ 100 ng per sample. This lack of a diurnal pattern in the sampled particles suggests that sources or processes that are responsible for these particles could have persisted throughout the day and night or could be from different processes that persisted both day and night. In contrast to this, the background period has a diurnal peak in estimated mass collected between 18:00 and 22:00 UTC, with sampled masses of ∼70 ng per sample. The minimum sample sizes occurred in the early morning, when averages reached as low as 16 ng per sample. Peaks in collected mass during the early afternoon could be linked to photochemically produced sources and appear to be unique to the background period. Assuming that the background contribution to the mass of particles remains constant between each time period, the average mass loading of ultrafine particles increased by a factor of 3 due to anthropogenic influence (Fig. S3).

The five most abundant negative ions, as observed in full mass spectra (Fig. S1) taken at the start of the wet season campaign, are attributed to CNO- (cyanate, m/z 42), C2H3O2- (acetate, m/z 59), HSO4- (bisulfate, m/z 97), Cl- (chloride, isotopes m/z 35 and 37) and HC2O4- (hydrogen oxalate, m/z 89). The six most abundant positive ions measured were attributed to NH4+(H2O) (ammonium hydrate, m/z 36), K+ (potassium, isotopes m/z 39 and 41), C3H10N+ (trimethyl ammonium, m/z 60), C5H7O+ (protonated 3-methylfuran, m/z 83), C5H8NO+ (m/z 98) and C7H9O2+ (m/z 125). We will refer to C5H8NO+ (m/z 98) and C7H9O2+ (m/z 125) collectively as “other” in our positive-ion-mode analysis, as these were minor components. The major isotopes of chloride were measured in order to understand the role chloride may have had on particle formation, with potential influence from marine aerosol and fungal spores (Pöhlker et al., 2012). Potassium (isotopes m/z 39 and 41) was measured during positive-ion-mode analysis to determine the potential influence of potassium-rich primary biological particles (China et al., 2016; Pöhlker et al., 2012). Additionally, potassium-rich particles have been linked to biomass burning, as potassium is found to be associated with soot carbon (Andreae, 1983; Pósfai et al., 2004). Mass-normalized ion abundances, defined as ion abundance divided by the collected sample mass, for the five most abundant negative ions displayed similar diurnal patterns within each period. During the anthropogenic period, peaks in mass-normalized ion abundance were observed for all measured species between 06:00 and 08:00 and 16:00 and 18:00. For the background period, there was no sharp peak observed between 16:00 and 18:00 for any of the five measured species, but there was a peak in the diurnal pattern between 06:00 and 08:00 for m/z 42, m/z 59 and m/z 89 (Fig. S4). Diurnal trends in mass-normalized ion abundances give little insight, per se, into sources of individual ions, but it is interesting to note that ion abundances are typically the lowest when the sample mass is largest. A potential reason for this is that TDCIMS is not sensitive to the specific compounds present in these ultrafine particles when the mass loading is highest. This could be true, for example, if refractory black carbon is the main constituent during the period of the highest sampled mass, as chemical ionization would be unable to detect these compounds. Since the diurnal patterns of all individual ions are similar, a comparison of ion fractions, defined as ion abundance divided by the sum of the total ion abundances measured at the time of analysis, provides a measurement of ion concentration in collected particles and shows distinct differences between the background and anthropogenic periods.

Figure 3a shows the trend in ion fraction for the five most abundant negative ions and four most abundant positive ions during the 10 d period of analysis. During the anthropogenic period, the observed bisulfate ion (m/z 97) fraction was larger than during the background period. Of the ions measured, bisulfate is the predominant indicator of urban influence. The bisulfate anion has been previously noted in TDCIMS analysis as a stable ion formed from the thermal desorption of particulate sulfate (Voisin et al., 2003), and it is likely that emissions from Manaus could serve as the major source for sulfate found at the T3 site. Thus as air masses during the anthropogenic period primarily traveled from, or to the south of, Manaus, bisulfate is expected to have a higher measured ion fraction. Additionally, in-basin emissions of various gaseous precursors like dimethyl sulfide and hydrogen sulfide could contribute to particulate sulfate of non-anthropogenic origin, as bisulfate was measured during the whole 10 d period of interest, even without observed direct influence from Manaus. When the bisulfate ion was the largest of the negative ions, the largest fractions of ammonium (m/z 36) and trimethyl ammonium (m/z 60) in the positive-ion mode were observed as well. Additionally, the largest chloride (m/z 35) signal was observed at the beginning of this period, reaching a maximum of about 10 % of the total ion fraction on 14 March. During the background period, the ion fraction of hydrogen oxalate (m/z 89) remained relatively constant, averaging 31 % ± 5 % of the total ion fraction. Diurnal patterns of these ion fractions, shown in Fig. 3b, show small diurnal variations for most of the observed ions. The diurnal pattern of m/z 42 (cyanate) peaks between 10:00 and noon and both m/z 59 and m/z 89 show slight decreases between 10:00 and noon as well. Roughly 70 % of measurements over both periods had potassium (m/z 39 and 41) ion fractions less than or equal to 20 % of the total positive-ion fraction, with few “potassium episodes” of higher abundance observed.

Interestingly, m/z 42 was the most abundant ion present in TDCIMS spectra. Due to its even mass-to-charge ratio, this ion almost certainly contains nitrogen. This ion distinguishes itself from other detected compounds by a peak in ion fraction during the morning (Fig. 3b). Prior TDCIMS measurements during the 2006 MILAGRO campaign in the Mexico City metropolitan area detected m/z 42 as a major ion fragment in sub-20 nm diameter particles; that ion was identified as cyanate (CNO-), which may be linked to isocyanic acid from biomass burning or industrial processes (Smith et al., 2008). The m/z 42 fragment observed in this study is not likely of anthropogenic origin, since this ion was observed during very clean periods when we expect anthropogenic emissions and biomass burning to be low. In addition, TDCIMS-measured m/z 42 during the dry season did not show an increase in ion intensity relative to the wet season (Smith, 2016), which one might expect if this ion were sourced to biomass burning. We hypothesize that this ion is cyanate (CNO-), which we associate with organic nitrogen related to aerosol formation from biogenic emissions of volatile organic compounds (VOCs). Natural emissions of amino acids, water-soluble organic species and other proteinaceous biogenic materials have been measured in the gas phase, particle phase and precipitation across the globe and have been estimated to account for as much as half or more of the bulk aerosol composition over the Amazon Basin (Artaxo et al., 1988, 1990; Kourtchev et al., 2016; Mace et al., 2003; Zhang and Anastasio, 2003). While all prior field measurements in the Amazon Basin have been made on particles larger than those measured in this study, similar sources may influence ultrafine-particle composition. If true, these observations suggest that organic nitrogen compounds play a crucial role in both ultrafine-particle formation as well as growth to large particles, which make this mechanism for particle growth climatologically important in this region.

Of the measured positive-ion species, m/z 83, linked to 3-methylfuran or other C5 oxidized volatile organic compounds, dominated the ion fraction in ultrafine particles. Methylfuran has been observed to be produced as a thermal decomposition product of isoprene-derived SOA via AMS measurements (Allan et al., 2014), a process that would likely also occur during TDCIMS analysis. Airborne observations in the Amazon suggest that isoprene SOA can be formed in the boundary layer under certain conditions, which is confirmed by these observations (Allan et al., 2014). Since this ion is a marker of isoprene epoxydiol (IEPOX) species present in the particle phase, this confirms a role for isoprene and isoprene derivatives in the growth of ultrafine particles. Little variability in the diel pattern for m/z 83 is observed, similar to other particle-phase measurements of IEPOX derivatives reported for the GoAmazon2014/5 campaign by Isaacman-Vanwertz et al. (2016). In that study, weak diurnal patterns for particle-phase isoprene oxidation products were also observed even while gas-phase concentrations of these species increased in the afternoon. It is important to note that this ion dominates the positive-ion fraction during both the anthropogenically influenced and background-influenced periods. Times that experienced lower fractions of m/z 83 had increased fractions of ammonium and trimethyl ammonium, which also coincided at times with larger amounts of measured bisulfate in the negative ions. The presence of larger fractions of particulate ammonia and amines at times with less influence from isoprene-derived species could indicate that both organic salt formation and uptake of isoprene-derived products are possible mechanisms of ultrafine-particle growth. The importance of organic salt formation in growth is consistent with prior TDCIMS measurements (Smith et al., 2010), although a quantitative comparison cannot be made, since this current study focuses on sub-100 nm diameter particles, whereas the prior study focused on size-resolved sub-15 nm ambient particles. One period of an elevated potassium ion ratio was observed at the end of the day on 22 March. To differentiate between potential sources of potassium in these ultrafine particles, whether they be of primary biological or biomass-burning influence, mass concentrations of black carbon during this 10 d period of interest were used to examine the extent of influence of biomass burning on the presence of potassium (Fig. S5). During the anthropogenic period, with significantly elevated concentrations of black carbon, a minimal potassium fraction was measured. At times of low black-carbon mass concentrations during the background period, like on 20 March, there was some fraction of potassium observed. During the period of the highest fraction observed on the night of 22 March, there were slightly elevated mass concentrations of black carbon. While partially elevated black-carbon mass concentrations on 22 March may be connected to the large potassium ion fraction, at times with even more significant biomass-burning influence, there was minimal potassium. The larger fraction of potassium observed during the background period, as opposed to the anthropogenic period, may be connected to potassium-rich biological particles or the rupturing of biological spores (China et al., 2016; Pöhlker et al., 2012). Of all wet season TDCIMS measurements during GoAmazon2014/5, roughly 14 % of measurements had potassium fractions greater than 0.1 (Fig. S6). Air masses on the evening of 22 March were traveling steadily from the Manaus area and coincided with about 5 mm of rain. High ambient concentrations of biological particles that could be sources of potassium are often associated with rainfall events (China et al., 2016). Rupturing of fungal spores, leading to the production of sub-100 nm fragments, was observed to occur after long exposures (above 10 h) of high relative humidity and subsequent drying, which are similar conditions to those on 22 March.

PCA was performed on TDCIMS and AMS measurements to provide insights into the possible drivers for ultrafine-particle formation. Figure 4 shows the results of this analysis. In these plots, positive correlations are shown in blue, while negative correlations are shown in red. The intensity of the color and eccentricity of the ellipse are an indication of the degree of correlation. Pale-colored circles (eccentricity approximately zero) show little to no correlation, narrow ellipses with a positive slope and darker blue color illustrate strong positive correlation, and narrow ellipses with a negative slope and darker red color show strong negative correlation.

Hierarchical clustering of these measurements results in three main clusters of related particle constituents. This represents a series of clusters where the species within each cluster covary, therefore being indicative, in this work, of similar particle characteristics, processes or sources. The first cluster, labeled “Cluster 1” in Fig. 4, grouped TDCIMS-derived cyanate (m/z 42), acetate (m/z 59), hydrogen oxalate (m/z 89), trimethyl ammonium (m/z 60) and 3-methylfuran (m/z 83); the second, labeled “Cluster 2”, clustered well-known covarying AMS derived constituents (Ulbrich et al., 2009); and the third, labeled “Cluster 3”, associated AMS-derived chloride with TDCIMS-derived chloride (m/z 35), bisulfate (m/z 97), ammonium hydrate (m/z 36) and potassium (m/z 39). The hierarchical cluster approach independently grouped and separated AMS measurements from TDCIMS measurements. While both represent composition measurements of the aerosol population, the differences between the size ranges of particles measured by AMS and TDCIMS techniques would lead to the anticipated differences in clustering. Comparing mass distributions estimated by size distribution measurements, the presence of particles larger than 100 nm would have a more significant contribution to the measured mass concentrations by AMS. In contrast, TDCIMS only measures sub-100 nm particles, representing a minor contribution to the total mass concentration. This observed separation between the clustering of AMS and TDCIMS measurements reinforces the importance of direct measurements of ultrafine particles, as opposed to bulk composition, in accessing the species and mechanisms responsible for new particle formation.

With respect to PCA performed on the two datasets, Cluster 1, which includes TDCIMS fragments typically linked to organic species (m/z 59, 89 and 83) and nitrogen species discussed previously (m/z 42 and 60), explains most of the variance and has the highest correlation with the first principal component. These species' high correlation with each other indicate similar sources, most of which can be associated with BVOC emissions. A prior TDCIMS laboratory study linked the acetate ion fragment (m/z 59) to particulate carboxylic and dicarboxylic acids (Smith and Rathbone, 2008), which have been linked to the photochemical oxidation of both biogenic and anthropogenic compounds (Winkler et al., 2012). During the wet season in the Amazon Basin, specific dicarboxylic acids and tricarboxylic acids have been identified and proposed to have been formed from the oxidation of semi-volatile fatty acids and terpenes (Kubátová et al., 2000). Hydrogen oxalate, measured as m/z 89, was one of the two most abundant organic ions measured in ultrafine particles at both an urban and rural site in Helsinki, Finland (Pakkanen et al., 2000). Hydrogen oxalate was noted to have relatively constant concentrations in ultrafine particles, similar to observations seen during the 10 d period of analysis for this study (Fig. 3). While Helsinki and the Amazon experience different conditions and meteorology, oxalate has been observed in both environments, possibly due to the heavy BVOC influence in both locales. In the positive-ion mode, 3-methylfuran, measured as m/z 83, has significant correlation to background linked negative ions. These species seem to be generally linked to the oxidation of various BVOCs, whether isoprene, for 3-methylfuran, or other terpenes (Allan et al., 2014). Finally, it should be noted that the clustering of the cyanate (m/z 42) with these organic ions provides further evidence that the source of this ion is likely clean, background chemistry rather than biomass burning. Additionally, TDCIMS-measured cyanate (m/z 42) is weakly and negatively correlated to AMS-measured nitrate. During the anthropogenic period (14 March through mid-morning 19 March), higher levels of inorganic nitrate were observed by AMS compared to the organic form (de Sá et al., 2018). This higher mass concentration of nitrate, attributed to inorganic nitrate as opposed to organic nitrate which would be more similar to TDCIMS-measured cyanate, should explain the slight negative correlation between the two.

Hierarchical clustering separates TDCIMS-measured ions into two clusters, with Cluster 3 including TDCIMS-derived bisulfate (m/z 97), chloride (m/z 35 and 37), ammonium hydrate (m/z 36) and potassium (m/z 39 and 41). The separation of this cluster suggests that these constituents are linked to different sources or atmospheric processes compared to those in Cluster 1, potentially with an anthropogenic origin, as both chloride and potassium and bisulfate have been linked previously to biomass burning and anthropogenic emissions, respectively (Allen and Miguel, 1995; Martin et al., 2010). As noted previously, the bisulfate anion is a stable ion formed from the thermal desorption of particulate sulfate (Voisin et al., 2003), and it is likely present in ultrafine particles via pollution emissions from Manaus. However, in-basin emissions of gaseous sulfate precursors, like dimethyl sulfide and hydrogen sulfide, could be linked to the measured bisulfate fraction during the entire 10 d period, with anthropogenic sources of sulfate increasing this background level during the anthropogenic period. In-basin chloride emissions could come from both biomass burning of common regional vegetation and long-range transport of marine ultrafine particles from the Atlantic Ocean under the influence of the trade winds (Allen and Miguel, 1995; Martin et al., 2010). The clustering of AMS chloride with TDCIMS species in Cluster 3 might suggest similar sources of chloride in both ultrafine particles and PM2.5. However, it is worth noting that AMS chloride also very weakly correlated with the other species measured by AMS. For this reason, its inclusion in this cluster indicates that AMS chloride is similar to TDCIMS-derived Cluster 3 species and also different enough so as not to cluster with the other AMS species. The production of potassium, which is potentially linked to rupturing of fungal spores and biomass burning, would have little correlation to other measured TDCIMS species, as the mechanism for the production of potassium is independent of SOA formation mechanisms. This ion is not generally associated to constant background sources, like TDCIMS species observed in Cluster 1, and may be associated with potential anthropogenic sources, like the bisulfate and chloride seen in Cluster 3. The clustering of TDCIMS ion abundances into two clusters suggests different sources and processes for these species, as there is little correlation between the species present in Cluster 1 to those present in Cluster 3.