Urban aerosol chemistry at a land–water transition site during summer – Part 1: Impact of agricultural and industrial ammonia emissions
This study characterizes the impact of the Chesapeake Bay and associated meteorological phenomena on aerosol chemistry during the second Ozone Water-Land Environmental Transition Study (OWLETS-2) field campaign, which took place from 4 June to 5 July 2018. Measurements of inorganic PM2.5 composition, gas-phase ammonia (NH3), and an array of meteorological parameters were undertaken at Hart-Miller Island (HMI), a land–water transition site just east of downtown Baltimore on the Chesapeake Bay. The observations at HMI were characterized by abnormally high NH3 concentrations (maximum of 19.3 µg m−3, average of 3.83 µg m−3), which were more than a factor of 3 higher than NH3 levels measured at the closest atmospheric Ammonia Monitoring Network (AMoN) site (approximately 45 km away). While sulfate concentrations at HMI agreed quite well with those measured at a regulatory monitoring station 45 km away, aerosol ammonium and nitrate concentrations were significantly higher, due to the ammonia-rich conditions that resulted from the elevated NH3. The high NH3 concentrations were largely due to regional agricultural emissions, including dairy farms in southeastern Pennsylvania and poultry operations in the Delmarva Peninsula (Delaware–Maryland–Virginia). Reduced NH3 deposition during transport over the Chesapeake Bay likely contributed to enhanced concentrations at HMI compared to the more inland AMoN site. Several peak NH3 events were recorded, including the maximum NH3 observed during OWLETS-2, that appear to originate from a cluster of industrial sources near downtown Baltimore. Such events were all associated with nighttime emissions and advection to HMI under low wind speeds (< 1 m s−1) and stable atmospheric conditions. Our results demonstrate the importance of industrial sources, including several that are not represented in the emissions inventory, on urban air quality. Together with our companion paper, which examines aerosol liquid water and pH during OWLETS-2, we highlight unique processes affecting urban air quality of coastal cities that are distinct from continental locations.
Inorganic salts, especially sulfate, nitrate, and ammonium, contribute a significant fraction of fine particulate matter (PM2.5) mass in the atmosphere. Ammonia (NH3) is an important component in this system due to its reaction with acidic species, especially H2SO4 (or HSO) and HNO3, to form secondary PM2.5. Volatility differences between H2SO4, HNO3, and NH3 result in a highly nonlinear system that is strongly influenced by the aerosol liquid water content and by small concentrations of nonvolatile aerosol species (Seinfeld and Pandis, 2016; Guo et al., 2018). The impact of NH3 on inorganic particulate matter formation has been extensively studied (e.g., Adams et al., 1999; Ansari and Pandis, 1998; Pinder et al., 2008; Bian et al., 2017). A common finding among these studies, and others, is that the NH3–H2SO4–HNO3–H2O system is characterized by “ammonia rich” and “ammonia poor” chemical regimes that produce substantial differences in aerosol composition and mass. These differences have direct implications for aerosol effects on public health (Pozzer et al., 2017; Paulot and Jacob, 2014), nutrient deposition and ecosystem health (Nenes et al., 2021; Bergström and Jansson, 2006), and global climate change (Turnock et al., 2019).
Emissions of the secondary aerosol precursors SO2, NOx, and NH3 directly affect regional PM2.5 concentrations (Pinder et al., 2007; Zhao et al., 2013). Air quality regulations in the US have substantially decreased SO2 and NOx emissions, leading to decreases in ambient PM2.5 (Hand et al., 2012a), while NH3 has remained largely unregulated. Reductions of NH3 emissions have been suggested as a cost-effective way to reduce PM2.5, as well (Pinder et al., 2007; Backes et al., 2016). Observations of wet deposition suggest that NH3 emissions have actually been rising over the past few decades (Keene et al., 2014). Globally, agricultural activity (from livestock and fertilizer application to crops) is the dominant source of NH3 emissions (Paulot et al., 2015; Pinder et al., 2006; Sutton et al., 2013). Synthetic fertilizer production has recently been identified as an intense local NH3 source (Van Damme et al., 2018), though its contribution to global emissions is likely small compared to volatilization from synthetic fertilizer applications (Bouwman et al., 1997).
While agriculture collectively emits a dominant fraction of NH3 globally, numerous other sources contribute to local or regional NH3 levels, especially in urban areas that are not in close proximity to major agricultural operations. Motor vehicles equipped with catalytic converters can reduce NO to NH3 in an undesired side reaction, resulting in significant NH3 emissions (Perrino et al., 2002; Sun et al., 2017; Kean et al., 2009). Anaerobic protein degradation produces NH3, as well, resulting in substantial atmospheric emissions from anthropogenic sources present in all urban areas, including landfills, composting, and wastewater treatment (Rittmann and McCarty, 2001; Artíñano et al., 2018). Numerous industrial sources emit NH3 (Meng et al., 2017), while natural sources (e.g., natural vegetation, wild animals, and large bodies of water) contribute to background NH3 levels (Paulot et al., 2015; Sutton et al., 2013). Biomass burning also emits NH3, though the effects are often seasonal and are most pronounced in regions with intense burning activities (Paulot et al., 2017). In the eastern US, biomass burning intensity is higher in spring and fall than in the summer (Washenfelder et al., 2015).
Urban air quality is controlled by emissions from multiple sectors, meteorology, and dynamic chemical processes that evolve throughout the day. Coastal cities often experience contributions from unique sources (e.g., ocean and shipping emissions), with chemical processes in the polluted marine boundary layer that are distinct from other regions in the atmosphere (e.g., de Gouw et al., 2005; Vutukuru and Dabdub, 2008). Further, meteorological processes associated with the land–water transition can exert a controlling effect on urban air quality that are absent in continental cities. One such phenomenon is the land–sea breeze (or bay breeze), which can prevent or reduce dispersion and contribute to enhanced secondary pollutant formation by recirculating primary urban emissions (Arya, 1999). This contributes to ozone exceedances and increased PM concentrations in highly populated coastal regions (Loughner et al., 2011; Caicedo et al., 2019). Understanding this process is critical since approximately 40 % of the US population lives in “Coastal Shoreline Counties” (NOAA, 2013). The purpose of the National Aeronautics and Space Administration (NASA) and Maryland Department of the Environment (MDE)-sponsored Ozone Water-Land Environmental Transitions Study (OWLETS-2) was to characterize the impacts of the Chesapeake Bay and its associated meteorological phenomena on air pollution formation and transport near Baltimore (Sullivan et al., 2019). In this study, we characterize secondary aerosol formation and sources of elevated NH3 measured at Hart-Miller Island, MD, a land–water transition site near Baltimore. In the companion paper, we analyze the effects of the Chesapeake Bay and elevated NH3 on aerosol liquid water content and aerosol pH during OWLETS-2 (Battaglia Jr. et al., 2021).
2.1 Site description
The OWLETS-2 campaign was a field study with multiple measurement platforms coordinating simultaneous water and land measurements of trace gases, aerosols, and meteorological parameters. This study presents analysis of inorganic aerosol composition and gas-phase ammonia measurements made at the Hart-Miller Island (HMI, Fig. 1) supersite. Hart-Miller Island is a state park located on the Chesapeake Bay, approximately 22 km from downtown Baltimore.
All measurements were made in the University of Maryland, Baltimore County (UMBC) trailer located on the southeastern side of the island (39.2421∘, −76.3627∘). Continuous measurements were conducted from 4 June to 5 July 2018. Several gaps in data collection occurred due to periodic power outages on the island.
Comparisons of the HMI measurements were made to two nearby inland sites: Beltsville and Howard University Beltsville (HUB, denoted HU-Beltsville hereafter), approximately 46 and 50 km southwest of HMI, respectively. Beltsville (39.0280∘, −76.8171∘) is a National Atmospheric Deposition Program Ammonia Monitoring Site (AMoN, http://nadp.slh.wisc.edu/amon/, last access: 28 July 2021) and was used for gas-phase NH3 comparisons. HUB (39.0553∘, −76.8783∘) is a regulatory monitoring site maintained and operated by MDE and was used for comparisons of speciated PM2.5 concentrations.
2.2 NH3 measurements
An AiRRmonia analyzer (RR Mechatronics, the Netherlands) was deployed for measurements of gas-phase ammonia (Norman et al., 2009). The analyzer was enclosed in a weatherproof aluminum box (non-temperature controlled) and placed on top of the UMBC trailer (∼4 m inlet height). The AiRRmonia uses a 5 cm stainless-steel inlet (i.d. = 0.2 cm) to minimize sampling artifacts associated with gas adsorption to inlet surfaces (Schmohl et al., 2001; Ellis et al., 2010; von Bobrutzki et al., 2010). The instrument samples air at a rate of 1 L min−1, giving a gas residence time of ∼0.01 s in the inlet. Ammonia in the sampled air is absorbed through a gas-permeable polytetrafluoroethylene membrane into an acidic aqueous stripping solution with close to 100 % collection efficiency (Wyers et al., 1993). NaOH is then added to raise the pH so that the collected NH3 (present as NH) is shifted to the NH3 form, facilitating transfer of NH3 through another gas-permeable membrane into a separate flow of deionized water. Dual conductivity detectors measure the difference in conductivity between the deionized water before and after this transfer, enabling quantification of sampled NH3 (Norman et al., 2009; von Bobrutzki et al., 2010). The temperature-dependent conductivity was calibrated approximately daily during OWLETS-2 using aqueous NH standards. The instrument’s operating principles, including gas collection efficiency and lack of response to aerosol NH, have been characterized previously (Wyers et al., 1993; Erisman et al., 2001). The NH3 measurements during OWLETS-2 were conducted with 10 min resolution.
Speciated inorganic PM2.5 measurements were made with a particle-into-liquid sampler (PILS) coupled to dual anion-cation ion chromatographs (IC, model 850 Dual IC, Metrohm), collectively referred to as the PILS-IC (Orsini et al., 2003). Ambient air was sampled at 16.0 L min−1 through a PM2.5 cyclone (URG Corp.) and two annular denuders in series (URG Corp.) to remove acidic (e.g., HNO3, HCl) and basic gases (e.g., NH3). The PILS sample was split and simultaneously analyzed for concentrations of both cations (Na+, NH, K+, Ca2+, and Mg2+) and anions (Cl−, NO, SO, and C2O) according to Valerino et al. (2017).
For anion analysis, the IC utilized a Metrosep A Supp 5 column (150 mm × 4.0 mm) with 1.0 mM NaHCO3 and 3.2 mM Na2CO3 eluent at a flow rate of 0.7 mL min−1. For cation analysis, the IC utilized a Metrosep C 4 column (150 mm × 4.0 mm) that was run with 2.5 mM HNO3 and 0.5 mM C2H2O4 eluent at a flow rate of 0.9 mL min−1. In the anion analysis, conductivity measurements were preceded by chemical suppression to reduce conductivity of the eluent. This configuration of the PILS-IC resulted in a limit of detection of 0.01 µg m−3 (air concentration) for each ion and a 5 min integrated sample every 20 min.
2.4 HYSPLIT model
The HYbrid Single-Particle Lagrangian Integrated Trajectory (HYSPLIT, https://www.ready.noaa.gov/HYSPLIT.php, last access: 28 July 2021) model was utilized to investigate source influences during OWLETS-2 (Stein et al., 2015). The model allows for air parcel trajectories, including the back-trajectory analyses used here, to infer regional source influences for the air masses sampled at HMI. High-Resolution Rapid Refresh (HRRR) 3 km meteorological data were used in generating back-trajectories. The uncertainty and limitations of the HYSPLIT model are worth noting here, especially in accounting for small-scale circulations. As a result, for all events discussed below, HYSPLIT trajectories were crosschecked with measured surface wind conditions and vertical wind fields measured from the meteorological station and a Doppler wind lidar (Leosphere Windcube 200S) deployed at HMI. Meteorological measurements of temperature, relative humidity, and surface wind speed and direction were made with the Vaisala MAWS201 meteorological station at 1 min resolution throughout the study.
During the OWLETS-2 campaign, gas-phase ammonia was characterized by unusually high concentrations. The average NH3 concentration (3.83 µg m−3) at HMI was more than 3 times greater than NH3 at the Beltsville AMoN site (1.20 µg m−3) during the summer of 2018 (Fig. 2a), a difference that was statistically significant at the 99 % confidence level (p value < 0.01). While average summertime NH3 shows an increasing trend at Beltsville, the concentrations measured at HMI in 2018 far exceed recent summertime levels at Beltsville. The HMI NH3 concentrations were also compared to two other AMoN sites (Fig. 1): Blackwater (∼ 90 km from HMI; 38.4449∘, −76.1112∘) and Arendtsville (∼110 km from HMI; 39.9231∘, −77.3078∘). Both of these sites are located in much closer proximity to strong agricultural NH3 emissions, as Blackwater is located on the Eastern Shore of Maryland and Arendtsville is located in southeastern Pennsylvania. Their average summer NH3 concentrations for 2018 were 57 % (Blackwater, 1.66 µg m−3) and 49 % (Arendtsville, 1.96 µg m−3) lower than those measured at HMI during OWLETS-2. In a previous deployment of the AiRRmonia analyzer at the Beltsville AMoN site (unpublished work), the average concentrations measured by the AiRRmonia over a 2-week span (6–20 September 2016) were within ∼0.5 µg m−3 of the colocated AMoN NH3 measurements, suggesting that systematic measurement differences are not responsible for the trends seen in Fig. 2a.
3.2 Impact on aerosol composition
Before investigating the sources of such high NH3 concentrations, we first characterize the effects on aerosol composition, because NH3 contributes significantly to secondary aerosol formation (Seinfeld and Pandis, 2016). Note that our companion paper analyzes the effects of the high NH3 concentrations on aerosol liquid water and acidity (pH) (Battaglia Jr. et al., 2021).
In the US, SO concentrations have decreased due to regulations and economic factors that have reduced SO2 emissions (Hand et al., 2012a). This trend is evident at HU-Beltsville (Fig. 2b), where the average summertime SO concentration has decreased by more than a factor of 8 since 2007 (8.23 µg m−3 versus 0.94 µg m−3). Note that the data shown in Fig. 2 only include the summer months (June, July, and August) to facilitate direct comparisons to the conditions during OWLETS-2. In contrast to the NH3 results, the average SO concentration at HMI (1.11 µg m−3) was quite close to the average concentration at HUB (0.94 µg m−3), a difference that was not significant at the 95 % confidence level (p value > 0.1). This suggests that the high NH3 concentrations at HMI did not have a large effect on particulate sulfate mass concentrations, consistent with the understanding of SO thermodynamics and results from a study in the southeast US (Weber et al., 2016). The agreement in SO concentrations between HMI and HU-Beltsville is unsurprising given the regional nature of SO2 emissions and the low spatial variability of SO levels in the eastern US (Beyersdorf et al., 2016).
While SO concentrations were typical for the region, the elevated NH3 did affect the particulate NH and NO concentrations. An ammonia-rich environment, defined when [Total Ammonia] > 2× [Total Sulfate], can facilitate NH4NO3 aerosol formation (Seinfeld and Pandis, 2016). The system measured at HMI was ammonia rich for approximately 25 % of the OWLETS-2 campaign.
As shown in Fig. 2c, the average NH concentration at HMI was more than 50 % higher than the summertime average at HU-Beltsville (0.38 µg m−3 and 0.23 µg m−3, respectively), which is statistically significant at the 99 % confidence level (p value < 0.01). The NH concentrations at HMI were higher than any of the past five summertime averages measured at HU-Beltsville, demonstrating the influence of elevated NH3. Aerosol NO was also significantly elevated at HMI compared to historical and 2018 summertime levels at HU-Beltsville (Fig. 2d). The HMI average NO (0.36 µg m−3) was more than a factor of 2 higher than at HU-Beltsville (0.14 µg m−3), which is also significant at the 99 % confidence level (p value < 0.01). The NO concentrations at HMI were also higher than typical summertime levels in the eastern US (Sickles II and Shadwick, 2008). The high average NO concentration during OWLETS-2 was heavily influenced by several peak events where the NO concentration exceeded 3 µg m−3 (Fig. S1).
Another notable aspect of the NO observed during OWLETS-2 was the diurnal profile (Fig. S2a). Formation of NH4NO3 is favored by both lower temperature and higher relative humidity (Stelson and Seinfeld, 1982). Thus, the observed midday peak in NO coincided with the most unfavorable meteorological conditions (Fig. 1 in Battaglia Jr. et al., 2021). More typical summertime diurnal profiles of NO in the eastern US exhibit a maximum around 06:00–07:00 LT and an afternoon minimum (Xu et al., 2015; Poulain et al., 2011; Weber, 2003; Wittig et al., 2004). The NO diurnal profile observed during OWLETS-2 indicates the important effect of the elevated NH3 during the campaign and will be discussed in more detail below.
NH and NO concentrations were elevated at HMI compared to the historical data (Fig. 2). In the eastern US, the PM2.5 mass fraction of NH4NO3 peaks in the winter with a minimum in the summer (Wittig et al., 2004). Ammonium sulfate, however, is consistently one of the largest fractions of PM2.5 mass in the eastern US (Hand et al., 2012b). For the OWLETS-2 study, the coefficient of determination (R2) for the linear correlation (least squares regression analysis) between 2× (SO + NO) and NH was 0.90 (Fig. 3), while the R2 value for the linear relationship between SO and NH was only 0.57 (not shown), indicating the importance of NH4NO3 and the ammonia-rich conditions during OWLETS-2.
Finally, it should be noted that NO concentrations can be affected by interactions between nitric acid and sodium chloride (Seinfeld and Pandis, 2016). This can have a large impact on aerosol composition in coastal urban areas (Athanasopoulou et al., 2008). However, sodium chloride aerosols, while observed periodically in the fine mode during the campaign, were not frequent enough or high enough in magnitude (max Na + Cl = 0.91 µg m−3) to suggest a strong influence of primary aerosol emissions from the Chesapeake Bay.
3.3 Characterization of ammonia sources
Source locations of the high NH3 events were investigated using the NOAA HYSPLIT model. Trajectories produced by the model were checked for consistency with vertical wind fields measured by Doppler wind lidar (when available, with the one discrepancy noted in Table 1). Back-trajectories were initialized from HMI (50 m altitude) at the time corresponding to each NH3 measurement. Air mass back-trajectories were run based upon a recent study’s estimate of 15 h for the average NH3 lifetime (Hauglustaine et al., 2014), though other studies have estimated much lower NH3 lifetimes for point sources (Dammers et al., 2019). Figure 4 shows the ensemble of all back-trajectories for the campaign colored by the measured NH3 concentration. Overall, the back-trajectory origins were consistent with predominant surface winds during the campaign. Figure 4 also shows that elevated NH3 concentrations were not limited to trajectories originating from a single direction or region.
A subset of the trajectories in Fig. 4 was further investigated to identify the potential sources of peak NH3 events. When both particle-phase and gas-phase ammonia were measured, total ammonia and gas-phase ammonia correlated strongly (R= 0.9927), showing that gas-phase ammonia is an effective tracer for total ammonia for this campaign. Eleven distinct events had peak NH3 concentrations above the 95th percentile (>7.96 µg m−3) for the OWLETS-2 study (Fig. 5). Back-trajectories for each event are shown in Fig. 6. Altitudes of all back-trajectories were below 1 km over the postulated source region.
Agriculture represents the largest source of atmospheric NH3 emissions globally (Sutton et al., 2013). Agricultural NH3 emissions stem from fertilizer and livestock management (Pinder et al., 2006). Previous studies have linked high livestock NH3 emissions with particulate nitrate formation (Xu et al., 2019; Paulot et al., 2016; Sorooshian et al., 2008). HMI is located in relatively close proximity to several areas of concentrated livestock production (Fig. 7). To the east and southeast of HMI, the Delmarva Peninsula (Delaware–Maryland–Virginia) is a large poultry producing region. The emissions from these chicken houses have been characterized by ground measurements (Siefert et al., 2004) and captured by satellite measurements (Warner et al., 2017). Additionally, there are large concentrations of dairy cows in southeastern Pennsylvania, also shown in Fig. 7. The NH3 emissions in this area are some of the highest in the country for dairy cows (Pinder et al., 2004b). While dairy cow populations are relatively minor in Maryland, poultry emissions could be a significant emitter in the same region of Pennsylvania where dairy cows are concentrated (Fig. S3). The back-trajectories identify events 1, 2, 4, 5, 6, 7, and 11 as having likely agricultural influence (Table 1), consistent with the agricultural hotspots identified here (Figs. 7, S3). Additionally, the source for event no. 3 is ambiguous, but has the potential to be the poultry sources discussed above.
While agricultural emissions were the likely source of many peak events, several events – including the highest NH3 concentration measured during the campaign – appear to have a nonagricultural origin. Specifically, the trajectories for event nos. 8–10 pass directly over the city of Baltimore and do not appear to intersect with any major agricultural sources in the 15 h prior to arrival at HMI. A number of urban and industrial NH3 sources are known, including motor vehicles (Bishop and Stedman, 2015; Sun et al., 2017) and fertilizer production plants (Van Damme et al., 2018). Ammonia is produced when proteins are broken down under anaerobic conditions (Rittmann and McCarty, 2001), causing landfills (Sutton et al., 2000), waste composting and processing (Sutton et al., 2013; Pagans et al., 2006), and wastewater treatment plants (Reche et al., 2015; Artíñano et al., 2018) to emit significant quantities of NH3, as well.
The contribution of traffic to event nos. 8–10 was likely quite small due to a combined R2 value of 0.201 between NH3 and CO for the duration of the three events (based on CO measurements colocated at HMI). NH3 and CO are correlated in vehicle emissions (Kean et al., 2009; Perrino et al., 2002); however, for these events, high NH3 was observed without a spike in CO. We acknowledge that order-of-magnitude differences in the atmospheric lifetimes of CO and NH3 would alter correlations downwind from sources co-emitting both pollutants, but in this case, the species with the longer lifetime (CO) did not show an enhancement during the NH3 events, suggesting mobile sources were not a significant factor here. The trajectories for event nos. 8–10 identify a cluster of potential industrial NH3 sources (Fig. 8).
The potential NH3 sources for event nos. 8–10 include the Back River Wastewater Treatment Plant (A in Fig. 8), the Patapsco Wastewater Treatment Plant (B), a W.R. Grace Chemical Production Facility (C), the Quarantine Road Landfill (D), a large-scale composting facility (E), and Yara Fertilizer Distributor (F). Of these facilities, only W.R. Grace (224.1 t yr−1) and the composting facility (1.03 t yr−1) are permitted to release NH3 by the state of Maryland (MDE, 2019a, b). However, the non-permitted sites are likely major NH3 emitters, based upon urban NH3 sources previously identified in the literature. It is likely that emissions from multiple sources collectively contributed to NH3 levels during these events; however, the potential sources are too close together to distinguish or estimate individual contributions.
It is important to note that numerous back-trajectories also passed over this cluster of industrial sources during times when NH3 was not elevated. However, event nos. 8–10 share characteristics that explain the high NH3 levels at HMI. The peak concentration of each event occurred between 07:00–08:00 LT (Table 1). Additionally, the events had extremely low wind speeds of 0.8, 0.7, and 0.6 m s−1, respectively, all well below the campaign average of 2.9 m s−1 (Table 1). These values were below the 10th percentile of all wind speeds measured at HMI during OWLETS-2.
Events 2 and 3 were cut short by power outages. Event 2 (one of the two events where wind lidar data were not available for crosschecking the back-trajectory) is the only event with a discrepancy between HYSPLIT (predicts wind direction coming from NNE) and observations (measured surface wind direction coming from E).
With such low wind speeds, transport time for the ∼18 km distance between the cluster of NH3 sources near downtown Baltimore and HMI would be ∼7–8 h for event nos. 8–10, suggesting that the original emissions occurred near midnight. Low wind speeds occurring at night correspond to the most stable atmospheric conditions and to a low boundary layer, which together enable elevated pollutant concentrations downwind of point sources (Arya, 1999). For example, event no. 10 had a peak NH3 concentration ∼15.5 µg m−3 higher than the campaign average (3.8 µg m−3). Under Pasquill–Gifford stability class F (nighttime, low winds), the required point source emission rate is 2 orders of magnitude lower (1 g s−1 vs. 172 g s−1) than it is under stability class B (slight daytime solar radiation, low winds) to give the same 15.5 µg m−3 NH3 enhancement at HMI. This illustrative example shows the potential for atmospheric stability to impact downwind surface concentration enhancement. Specifically, for this study, urban sources with moderate NH3 emissions can have a profound effect on downwind NH3 levels under the most stable atmospheric conditions.
Further, event nos. 8–10 also occurred shortly before onsets of the Chesapeake Bay breeze. The convergence between an offshore synoptic flow and the breeze creates a period of stagnation or calm winds that favor the accumulation of pollutants (Caicedo et al., 2019; Loughner et al., 2014). Additionally, the early morning occurrence of event nos. 8–10 also suggests that a low dilution volume as the marine boundary layer is only beginning its convective regime (Stull, 1988). Combined, calm winds and relatively shallow boundary layers are important factors contributing to the high NH3 concentrations.
Natural sources of NH3 can represent the dominant source of emissions in some regions (Paulot et al., 2015; Sutton et al., 2013). The Chesapeake Bay can be a source or sink for NH3 in the summertime (Larsen et al., 2001); however, the emission factors reported by Larsen et al. (2001) suggest a relatively minor influence of Chesapeake Bay emissions compared to the agricultural and industrial sources discussed above.
3.4 Temperature effects
Temperature plays an important role in NH3 emissions from fertilizer and animal waste (Robarge et al., 2002; Pleim et al., 2013). This contributes to strong seasonal and diurnal profiles of agricultural NH3 emissions (Warner et al., 2017; Zhu et al., 2015; Pinder et al., 2004a). The average diurnal profile of NH3 (Fig. 9a) shows enhanced concentrations between the hours of 07:00–15:00 LT, consistent with temperature-driven emissions. Overall, NH3 concentrations rose with increasing temperature (Fig. 9b); however, there was a lot of scatter in the data (R2=0.05 for individual (10 min) measurements of NH3–temperature over the entire campaign). In the absence of strong local sources of NH3 emissions, ambient observations are most impacted by transport. At HMI, this includes diverse source sectors from different areas that correspond to various time lags in emission to observation. This confounds strict interpretation of temperature-dependent emission relationships.
3.5 Deposition effects
Several factors likely explain why the NH3 concentrations observed at HMI were more than 3 times higher than those observed at Beltsville (Fig. 2a). Due to differences in proximity to the city of Baltimore (Beltsville is ∼45 km from downtown Baltimore) and to the Chesapeake Bay (e.g., bay breeze circulation), Beltsville was not affected by the identified industrial areas as severely as Hart-Miller Island. Further, when the wind direction may have facilitated transport from downtown Baltimore to Beltsville, the atmospheric conditions were not typically stable, giving rise to much lower downwind concentrations. However, the trajectory analysis (not shown) indicates that Beltsville frequently received air masses that had recently passed over the agricultural areas of the Delmarva Peninsula, the most common source of extreme NH3 concentrations at HMI (Table 1).
The most likely explanation for the higher concentrations at HMI is a dramatic difference in the bidirectional flux of NH3 during transport to each site. The path from the Delmarva Peninsula to Hart-Miller Island consists primarily of transport over water (the Chesapeake Bay), while the path for transport to Beltsville includes significantly more time and distance over land (∼40 km). The dry deposition velocity of gases is typically lower over water than over land, especially forested regions like the land surrounding the Beltsville AMoN site (Li et al., 2019). Additionally, the Chesapeake Bay can be a net source of NH3 during the summer (Larsen et al., 2001), suggesting deposition can be, on a net basis, quite small over the body of water. A recent modeling study found that reactive nitrogen undergoes much higher rates of dry deposition to the coastline bordering the Chesapeake Bay compared to rates over water (Loughner et al., 2016). The NH3 measurements at Beltsville are 2-week integrated samples, precluding a direct comparison to the HMI measurements and quantitative estimates of NH3 lost to dry deposition during transport. However, dry deposition of NH3 is a key uncertainty in accurate NH3 predictions (Pleim et al., 2013), so future studies should examine this question directly. The dry deposition of NH3 and HNO3 are affected by the aerosol liquid water content and particle pH (Nenes et al., 2021), and this will be analyzed in our companion paper.
Semicontinuous measurements of aerosol chemical composition and gas-phase NH3 were carried out during summer 2018 as part of the OWLETS-2 field campaign. The measurement site was located in close proximity to the land–water transition between the Chesapeake Bay and downtown Baltimore, MD. Sulfate levels were in line with historical trends and with concentrations measured at the same time in other locations near Baltimore. However, average aerosol NO and NH concentrations were significantly elevated compared to the average concentrations at a regulatory monitoring site ∼45 km away. The elevated aerosol concentrations were likely driven by gas-phase NH3, as higher background levels and episodic spikes contributed to average NH3 concentrations that were more than 3 times higher than the average levels measured at a nearby (∼45 km) AMoN site.
An array of sources likely contributed to the elevated NH3 concentrations. Agricultural emissions from poultry operations in the Delmarva Peninsula and dairy cattle in southeastern Pennsylvania were the most frequent sources of high NH3 at HMI. Low dry deposition velocities over the Chesapeake Bay enabled efficient transport of NH3 (and likely HNO3, as well) to the site. Under stable atmospheric conditions, industrial NH3 emissions from a cluster of sources near downtown Baltimore also contributed to several peak NH3 events, including the highest NH3 concentrations measured during OWLETS-2 (>19 µg m−3). These observations demonstrate the complex interplay between emissions, transport, and meteorology in affecting urban aerosol chemistry. Our companion study examines the effects of the unique meteorology and high NH3 concentrations on aerosol liquid water content and acidity (pH) (Battaglia Jr. et al., 2021).
Prior studies have shown that sulfate is regional in nature in the eastern US, exhibiting low spatial variability over tens of kilometers (Beyersdorf et al., 2016). Our results are consistent with these findings, suggesting that meteorological phenomena such as the bay breeze circulation or urban heat islands (Battaglia et al., 2017) do not substantially alter sulfate levels in this region. On the contrary, our results suggest strong gradients of reactive nitrogen species in the aerosol and gas phases, which will also produce periodic spatial gradients (including episodic spikes) in PM2.5 mass. The relatively short duration of these events and their dependence on proximity to water suggests they may not be well captured by regulatory monitoring (or longer-term monitoring for deposition networks). These results likely have implications for atmospheric chemistry and air quality in other coastal cities, including those outside of the eastern US. Our results suggest that analyses of urban air quality may be more illuminating if the urban areas are, themselves, segregated into coastal and inland locations. For example, the AeroCom study evaluated a number of global aerosol models using predictions in urban and remote locations as key indicators of model predictive skill (Tsigaridis et al., 2014). Our results highlight important differences in sources and processes affecting coastal versus inland urban areas that may have a determining effect on aerosol composition and concentrations.
Publicly available code (https://github.com/AirChem/HYSPLITcontrol, Wolfe, 2021) was used to run back-trajectories in bulk and scale their color by user-input data (code courtesy of Glenn Wolfe, NASA/GSFC and UMBC/JCET).
Data are available at https://www-air.larc.nasa.gov/cgi-bin/ArcView/owlets.2018 (NASA, 2021).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-21-13051-2021-supplement.
CJH, AGC, and RD conceived the analysis and study participation. MAB Jr., NB, and KB collected and analyzed the PILS-IC and NH3 data. NB and CJH conducted the trajectory and source identification analyses. VC and AGC provided analytical input and interpretation. NB and CJH wrote the article. All authors provided feedback and revisions to the article.
The contact author has declared that neither they nor their co-authors have any competing interests.
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Annmarie G. Carlton and Christopher J. Hennigan acknowledge funding from the National Science Foundation, AGS-1719252 and AGS-1719245. Ruben Delgado and Vanessa Caicedo acknowledge support by the Maryland Department of the Environment (contract no. U00P8400651). Nicholas Balasus and Katherine Ball received support through the NOAA Office of Education, Educational Partnership Program with Minority Serving Institutions (EPP/MSI) and the Cooperative Science Center for Earth System Sciences and Remote Sensing Technologies (grant no. NA16SEC4810008).
This research has been supported by the National Science Foundation (grant nos. AGS-1719252 and AGS-1719245), Maryland Department of the Environment (contract no. U00P8400651), and the National Oceanic and Atmospheric Administration (grant no. NA16SEC4810008).
This paper was edited by James Allan and reviewed by two anonymous referees.
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