Rapid industrial growth and urban expansion in South Korea over the past several decades has been accompanied by increased exposure to criteria pollutants such as ozone (O3), particularly in the Seoul Metropolitan Area (SMA) (Jo and Nam, 1999; Ghim and Chang, 2000; Chang et al., 2017; Kim and Lee, 2018; Seo et al., 2018; Fleming et al., 2018). Exposure to high levels of O3 is deleterious to human health and the environment, and has been linked to increased human mortality and decreased crop yields (Haagen-Smit et al., 1952; Heck et al., 1982; Chameides et al., 1999; Kim et al., 2004; Jerrett et al., 2009). Fleming et al. (2018) noted that the annual fourth-highest maximum daily 8-hour average (MDA8) O3 value increased at an average rate of 2 ppbv per year between 2000–2014, and the number of days with 8-hour O3 values greater than 70 ppbv increased by up to two days per year across South Korea. While ambient O3 levels in South Korea have been increasing for some time, recent work by Jung et al. (2018) suggests that the rate of increase has risen in recent years. Broader analysis of trends across greater East Asia has shown that O3 values throughout the region have been increasing in the past decade, raising questions about the influence of regional versus local emissions on air quality in the SMA (Chang et al., 2017). However, the trends noted by Fleming et al. (2018) and Chang et al. (2017) were significantly more prevalent at urban sites in South Korea than at rural sites, indicating that, while long-range transport may contribute to increasing background levels of O3, local emissions must be addressed in order to improve air quality. In this work, data collected during the Korea United States Air Quality Study (KORUS-AQ) are used to better understand the primary drivers for O3 in the SMA.
There are no primary emission sources of O3, and instead it is formed through the photochemical interaction between emissions of volatile organic compounds (VOCs) and nitrogen oxides (NOx = NO + NO2). Therefore, strategies to reduce O3 in the SMA must focus on reducing local and regional emissions of these precursor species. However, O3 chemistry is complex and varies non-linearly with respect to precursor concentrations, and therefore a detailed understanding of the sensitivity of local O3 formation to changes in the precursor environment is essential for drafting effective mitigation strategies. This non-linear response of O3 to concentrations of its precursors results in the presence of two distinct photochemical regimes, often referred to as “NOx-limited” and “radical-limited” (also called “VOC-limited” due to the relationship between VOCs and radicals) (Sillman et al., 1990; Kleinman, 1994). Understanding local O3 sensitivity (i.e. whether O3 formation is NOx-limited or radical-limited) is a crucial first step for drafting targeted mitigation strategies. Formation of O3 in the background troposphere is typically NOx-limited, while the urban areas around many megacities are often radical-limited (Duncan et al., 2010). However, these terms should not be taken to imply either/or solutions for ozone mitigation. For instance, megacities are not radical-limited because of minimal VOC emissions, but rather because of an overabundance of NOx, making the term “NOx-saturated” a more appropriate term. In such “NOx-saturated” environments, reduction of NOx is necessary to achieve long-term ozone reduction but would be expected to lead to short-term ozone increases without concurrent action to reduce VOC emissions. In this work, the terms “radical-limited”, “VOC-limited”, and “NOx-saturated” are taken to have the same meaning, and we choose to use “radical-limited” for simplicity.
While classifying regional O3 production as NOx-limited or radical-limited is an important first step, we must note that “VOCs” refers to a collection of hundreds of distinct trace gases arising from a variety of anthropogenic and natural sources, each with unique rates of reaction with OH and unique radical yields upon oxidation. Therefore, in radical-limited (i.e. VOC-limited) environments, investigating the sensitivity of O3 to individual VOCs or subsets of similar VOCs is necessary for developing mitigation strategies that target emissions sectors that contribute disproportionately to local O3 formation.
Effective O3 control strategies rely on accurate understanding of how ambient O3 levels would respond to reductions in precursor emissions; thus, potential biases or uncertainties from model-based and observation-based studies must be taken into consideration. 3D models that include emissions, transport, and chemistry are well-suited for exploring the response of simulated O3 to reductions in modeled emissions, but are subject to large uncertainties in many parameters (particularly emissions) that lead to uncertainties in simulated O3 and the simulated dependence of O3 on its precursors (Sillman, 1995, 2003; Sillman et al., 1998; Zhou et al., 2013; Choi and Souri, 2015; Goldberg et al., 2016). Ground-based studies that make use of O3 sensitivity indicators (as described in Sillman and He (2002) and Schroeder et al. (2017)) have the advantage of making direct observations of the real atmosphere, but may be limited to one location, making it difficult to understand how representative they are of a broader region (Thornton et al., 2002; Mao et al., 2010; Edwards et al., 2013; Ren et al., 2013). Furthermore, recent work has highlighted the presence of vertical gradients in O3 precursors within the boundary layer, suggesting that significant bias can arise if surface observations are used to infer integrated rates of O3 production throughout the boundary layer (Zhang et al., 2016). Airborne studies, on the other hand, provide measurements of O3 and its precursors over large geographical areas, allowing for calculation of O3 production rates and O3 sensitivity at local and regional scales across vertical gradients (Kleinman et al., 2001, 2002; Mazzuca et al., 2016; Schroeder et al., 2017). This work uses data collected onboard the NASA DC-8 aircraft during the Korea-United States Air Quality Study (KORUS-AQ; May 2–June 11, 2016) to explore gradients in O3 and its chemical precursors in the SMA, and uses an observationally-constrained box model to quantify the response of simulated O3 production rates to perturbations in the precursor environment. While much can be learned from analysis of box model calculations, care must be taken to ensure that the constraints used to drive the model and the underlying chemical mechanism within the model adequately represent conditions in the SMA. For this reason, a large portion of this work (Section 4) is dedicated to analysis of model performance against a number of metrics, including comparison of model-calculated abundances of secondary “test species” to observations, and comparison of calculated rates of O3 production to observed changes in O3.
To help place the KORUS-AQ observations into context, it is useful to first examine the distribution of surface ozone observed by the AirKorea network of air quality monitoring sites. KORUS-AQ was conducted during the climatological peak of O3 season in South Korea that occurs during the pre-monsoon period in late spring/early summer, typically during May and June (Ghim and Chang, 2000; Jo et al., 2000; Kim et al., 2006). Therefore, the timing of the field deployment is germane to exploring spatiotemporal tendencies in O3 and conducting policy-relevant analysis of the key drivers of O3 formation.
The SMA has a population of approximately 25 million, divided into three main regions: Urban Seoul (population 10 million), the Incheon metropolitan city (population 3 million), and the surrounding Gyeonggi province (population 12 million). Figure 1 shows the location of air quality monitoring sites maintained in these three regions by the National Institute of Environmental Research (NIER) as part of the larger country-wide AirKorea network. Statistics for observations across these sites are summarized in Table 1. Percentile statistics for sites across the three regions are provided for MDA8 O3, associated levels of Ox (O3 + NO2), and number of exceedance days in each region. Exposure to high O3 levels is significantly greater for sites in Gyeonggi province with monitors recording MDA8 O3 values in excess of the Korean standard of 60 ppbv roughly half of the time. Seoul and Incheon experience such values, but only violate the Korean standard a little over a quarter of the time with lower O3 values that tend to be about 10 ppbv less than those observed in Gyeonggi province. This difference can be better understood when looking at statistics for the associated Ox values, which show Seoul to have values that run a few ppbv higher than Gyeonggi due to the proximity to greater NOx emissions. While Incheon values of Ox are still lower than Gyeonggi, the regional difference in Ox is smaller than that for O3. Based on these statistics, the greater number of exceedance days for Gyeonggi province can be attributed mainly to the lower NOx levels in comparison to Seoul and Incheon rather than higher overall oxidant levels. These observations drive the motivation for this work, which broadly aims to answer the following two questions: 1) Which O3 precursor species are the primary drivers of O3 production in the SMA? And 2) What mitigation strategies would be most effective for achieving reductions in O3 across the SMA? This work uses measurements made onboard the NASA DC-8 aircraft during KORUS-AQ and observation-based modeling to explore these questions and provide policy-relevant information about the local photochemical environment.
|Location (color in Fig. 1)||Urban Seoul (red)||Incheon (yellow)||Gyeonggi (blue)|
|Percentile Statistics for MDA8 O3 at AirKorea monitors (units: ppbv)|
|Percentile Statistics for MDA8 Ox (O3 + NO2) at AirKorea monitors (units: ppbv)|
|Number of Exceedance Days (at least one monitor with MDA8 O3 > 60 ppbv)|
KORUS-AQ was a multi-agency, multi-platform international field campaign that took place in South Korea from May 2–June 11, 2016. As part of KORUS-AQ, the NASA DC-8 aircraft performed 20 local research flights over South Korea. A map showing all local DC-8 flights during KORUS-AQ is shown in the top panel of Figure 2. During most research flights, the DC-8 flew a standard route over the SMA that was repeated during the morning (~9:00 local time), midday (~12:30 local time), and afternoon (~3:30 local time). This route is shown in the bottom panel of Figure 2, which descends over the city and passes over two instrumented supersites. The descent over the city began from ~2.5 km at the northern end of urban Seoul, passing over the Olympic Park site at ~0.5 km before coming within meters of the surface over the runway of Seoul Air Base, located about 8 km south of Olympic Park. From Seoul AB, the DC-8 proceeded at low altitude to pass over the Taehwa Forest research site at ~0.3 km before performing a wide ascending spiral up to ~10 km in the area to the east of Taehwa. Sampling along this route was performed on fifty-five occasions under a wide variety of air quality conditions. This provides a strong statistical basis for exploring the spatial and temporal variability over short term time scales (i.e. diurnal variability within one day) and relatively long time scales (i.e. day-to-day variability over the study period). The primary objective of KORUS-AQ was to collect measurements that would facilitate a better understanding of the chemical and physical processes that control air quality over South Korea, with an emphasis on collecting observations that could improve satellite-based remote sensing of air pollution. Because of this, the majority of flights during KORUS-AQ were conducted during sunny or partly cloudy conditions, which are also conducive to O3 formation. Much of the KORUS-AQ study period was characterized by consistent high pressure with relatively weak synoptic flow. Under these conditions, characterized by stagnant airmasses in the morning and a building westerly sea breeze through the afternoon, Taehwa forest acted as a receptor site for outflow from urban Seoul.
The instrument payload of the DC-8 was designed to allow for detailed studies of gas phase and condensed phase chemical processes. The subset of airborne measurements that are directly related to this work include trace gases (O3, NO, NO2, CO, water vapor, CH2O, PAN, H2O2, HNO3, and speciated VOCs), meteorological variables, and photolysis rates. All DC-8 measurements used in this work are summarized in Table 2.
|Instrument Name||Species Measured||Reference(s)|
|Diode Laser Hygrometer (DLH)||water vapor||(Diskin et al., 2002)|
|Differential Absorption CO Measuerment (DACOM)||CO, CH4||(Sachse et al., 1991)|
|NOxyO3 Chemiluminescence||O3, NO, NO2||(Weinheimer et al., 1994)|
|Compact Atmospheric Multi-species Spectrometer (CAMS)||CH2O, C2H6||(Weibring et al., 2010; Richter et al., 2015)|
|Proton Transfer Time of Flight Mass Spectrometer (PTR-TOF-MS)||methanol, acetone + propanal, isoprene, MVK + MACR, benzene, toluene, C8 aromatics||(Muller et al., 2014)|
|Whole Air Sampler (WAS)a||C2-C10 alkanes, C2-C4 alkenes,
C6-C9 aromatics, isoprene
|(Colman et al., 2001)|
|Georgia Tech Chemical Ionization Mass Spectrometer (GTCIMS)||PAN||(Slusher et al., 2004)|
|California Institute of Technology Chemical Ionization Mass Spectrometer (CIT-TOF-CIMS)||H2O2, CH3OOH||(Crounse et al., 2006)|
|CCD-Based Actinic Flux Spectrometers (CAFS)||4π sr actinic flux and derived photolysis frequencies||(Shetter et al., 1999)|
The observationally-constrained NASA Langley Research Center (LaRC) 0-D time-dependent photochemical box model was used to simulate ozone photochemistry during KORUS-AQ. The model was constrained by coincident observations of trace gases such as O3, NO, CO, CH4, CH2O, water vapor, and non-methane hydrocarbons; by meteorological parameters such as temperature and pressure; and by photolysis rates derived from actinic flux observations. The model calculates the diurnal steady-state profiles of radicals and other computed species for each set of measurements along the flight path (Crawford et al., 1999; Olson et al., 2001, 2006). In effect, the model is integrated forward in time until all calculated species exhibit a reproducible diurnal cycle (i.e. convergence is met for each calculated species). Values are extracted for the specific time of the flight measurement to enable the calculation of instantaneous ozone production rates associated with the measurements along the flight path. During the simulated diurnal cycle, all constraining species are held constant. NOx requires special treatment to allow interconversion between NO, NO2 and other short-lived reactive nitrogen species during the diurnal cycle. In this case, the total abundance of NOx is held constant but calculated to be consistent with the observed NO mixing ratio at the time of the measurement. The diurnal variation of photolysis frequencies is calculated for clear-sky conditions and scaled by the ratio of observed-to-clear-sky values at the time of the measurement. The most recent update to the chemical mechanism, including a complete list of all reactions used in the model is provided in Schroeder et al. (2017); however, updates to the aromatic chemistry mechanism have been made and are described later in this section.
In highly polluted conditions, the appropriateness of the steady-state assumption becomes less valid. For instance, Fried et al. (2011) demonstrated that model estimates of CH2O can be biased in pollution plumes when short-lived species dominate the model photochemistry, e.g., highly-reactive VOCs such as biogenic isoprene or alkenes from industrial sources. Under such conditions, using observations to constrain CH2O and other important radical reservoirs instead of calculating them will improve model calculations of the radical pool responsible for ozone production. The intricacies of the steady-state assumption will be explored further in Section 4 using comparisons of fully-constrained and minimally-constrained model runs. Additional model uncertainties arise from uncertainties in measured constraints and uncertainties in kinetic and photolytic rates.
Model inputs for each flight were derived from DC-8 1-s merges (available at https://www-air.larc.nasa.gov/missions/korus-aq/index.html). However, creating 1-s model inputs from these DC-8 1-s merges involved many steps to maximize the number of data points that could be run by the model. At a minimum, The LaRC 0-D photochemical box model must be constrained by coincident measurements of CH4, CO, NO, O3, H2O, and photolysis rates. To maximize the number of points that could be run by our model, an iterative median smoothing process was performed to fill in missing data points for these species. Missing data were replaced with the median of the surrounding ±3n data points, where n = 1, 2, 3, 4. In effect, this allows for the smallest smoothing window possible to be used for each missing value. First, we attempted to replace missing values with the median of the surrounding ±3 data points (i.e. n = 1), under condition that at least half of the data points within the window were not missing themselves. If that condition was not met, median smoothing was attempted with a window of the surrounding ±6 data points (i.e. n = 2), onwards until a final smoothing window of ± 12 data points (i.e. n = 4) was reached. Flying at an altitude of 1 km, the DC-8 would travel a distance of about 3 km in 24 seconds (i.e. the time duration of the maximum smoothing window, n = 4), and a maximum vertical distance of about 120 meters (the DC-8 typically ascended/descended at a maximum rate of 5 m/s). For the subset of KORUS-AQ data highlighted in this paper, i.e., less than 2 km altitude over the SMA (36.9–37.73 N, 126.65–127.83 E), this smoothing process contributed to 8% of the CO and CH4 observations (consistent with the frequent calibration of the instrument every 5 min), 2.6% of the water vapor observations, and less than 2% of the O3 and NO observations. This enabled just over 77,000 unique calculations accounting for 80% of the DC-8 flight time over the SMA.
This median smoothing process was also applied to the following non-critical constraints: CH2O, PAN and methanol. These are species that can be calculated by the model if not available to constrain the calculations. Smoothed data contributed to roughly 4% of CH2O, 9% of PAN, and less than 2% of methanol data used in the calculations enabling constraint of these species for all but a handful of model runs. In the case of H2O2 and HNO3, the smoothing process was not effective in adding much additional information, but observations were still available to constrain over 80% of the model runs. Fortunately, constraining these species had a negligible effect on calculations for the conditions encountered over the SMA during the study period (see discussion in Section 4).
A final step in preparing the model inputs required special consideration for non-methane hydrocarbons. Fortunately a subset of important hydrocarbons were measured at 1 Hz: C2H6 by CAMS and aromatics and isoprene by PTR-TOF-MS (see Table 1 for complete list). The large number of other hydrocarbon compounds were derived from whole air samples collected at discrete time intervals (see Table 1 for details). For these species, “pseudo” 1 Hz interpolated values were derived using 1 Hz measurements of C2H6. Taking the ratio of each WAS measurement of C2H6 to the average of 1 Hz measurements during the WAS integration time resulted in a small correction factor for each sample. Taking these correction factors, the full timeline of 1 Hz C2H6, including time gaps between WAS samples, was normalized by applying the average ratio between consecutive samples from the middle of one sample integration period to the next. This “adjusted 1 Hz ethane” was then used to derive 1 Hz inputs for other WAS species having anthropogenic sources. For example, a “pseudo” 1 Hz propane input was derived by taking the propane-to-ethane ratio for each WAS measurement. These ratios were then applied to the “adjusted 1 Hz ethane” again using the average ratio between consecutive WAS samples from the middle of one sample integration period to the next. This scheme was applied to derive 1 Hz inputs for lumped C4+ alkanes, ethene, lumped C3+ alkenes, ethyne, and benzene. Similar to the correction of 1 Hz C2H6, isoprene measurements from WAS canisters and 1 Hz PTR-TOF-MS data were used to derive an “adjusted 1 Hz isoprene” input. PTR-TOF-MS measurements of toluene and C8 aromatics were found to be in very good agreement with WAS measurements, so 1 Hz measurements of these species were used as-is for model inputs. Remaining VOC inputs, such as methanol and acetone, were only measured by PTR-TOF-MS and therefore used as-is for model inputs.
Model calculations of the free radical species that mediate ozone production allowed for the determination of instantaneous rates of net ozone production, P(O3), with individual terms given in the equation below.
The first two terms represent ozone formation from the conversion of NO to NO2 by hydroperoxy (HO2) radicals and the numerous organoperoxy (RO2) radicals resulting from hydrocarbon oxidation. Loss terms include the reaction of O1D from ozone photolysis with water, direct reaction of ozone with OH and HO2, reaction of NO2 with OH to form nitric acid (an indirect ozone loss via odd oxygen, Ox ≡ O3 + NO2), and ozonolysis reactions with hydrocarbon species.
As noted above, a minor adjustment to the model mechanism was made in response to the dominance of C7+ aromatic compounds in the SMA. In previously modeled environments, including airborne field campaigns over remote areas and polluted cities in the USA, aromatic species had never played a dominant role. For example, the mean mixing ratio of C7+ aromatics below 1 km over Seoul during KORUS-AQ was a factor of five higher than observed below 1 km over Houston during the DISCOVER-AQ airborne campaign (Summer 2013). This led to scrutiny of the OH reaction rate constant for the lumped C7+ aromatic compounds (AROM) when initial model calculations produced unrealistic results for peroxyacetylnitrate (PAN) and CH2O, indicating that the modeled radical environment (and modeled rate of P(O3)) was also unrealistic. Specifically, using the original OH rate constant for C7+ aromatics led to model over-prediction of PAN in Seoul by a factor of 10–15 and CH2O by a factor of 2–3. The rate constant, one of only a few still based on the Lurmann et al. (1986) lumped hydrocarbon mechanism, was found to significantly overpredict the rate of aromatic oxidation by OH when considering current literature for toluene and higher aromatic reaction rates. To best represent aromatic oxidation, the rate constant for AROM + OH was updated to take the following form:
This equation combines the rate constant for toluene with a simple scaling factor, A, accounting for the ratio of C8 aromatics to toluene for a given model run. The calculation of A took the following form:
The scaling factor of 2.43 was derived by assessing the relative OH reactivity of toluene versus C8 aromatics (kC8 aromatics + OH/kToluene + OH) for the mean mixing ratios of aromatics measured in the whole air samples. For a scaling factor of A =1.4 (median value for calculated over Seoul) and a temperature of 298 K, the revised rate constant is about 50% lower than the original rate constant. In addition, the stoichiometric yields of glyoxal and methyl gloxal from C7+ oxidation under high-NOx conditions have been adjusted from 0.18 and 0.72 to 0.27 and 0.3 to better-reflect results from chamber experiments (Tuazon et al., 1984; Smith et al., 1998) and to better agree with lumped chemical mechanisms used in 3D models, such as CAM-Chem (Louisa Emmons, private communication, 2018). These changes combined to lower the calculated P(O3) below 2 km over the SMA by an average of 20%, but at low altitudes over Seoul, where observations of C7+ aromatics were highest, these changes resulted in up to a 65% decrease in calculated P(O3). Outputs from all box model simulations are available on the KORUS-AQ archive: https://www-air.larc.nasa.gov/cgi-bin/ArcView/korusaq?MODEL=1.
To provide confidence in model-calculated rates of P(O3), which cannot be directly observed, an objective assessment of model performance is enabled by observed species that can either be used to constrain the model as an input or be calculated to be in photochemical steady state. Comparison of calculated and observed values for these test species can provide important insights on the aspects of the photochemistry that are being well represented and the sensitivity of the model to aspects that are not well represented. Limitations of the model are exacerbated for species with longer lifetimes, which are less likely to in photochemical steady state, and conditions under which physical processes such as transport, deposition, or wet removal are dominating over photochemistry. It is also useful to have a large number of observations over which to test model performance as there are many conditions that can perturb local steady state for individual runs but not induce a bias in the overall statistics. For instance, measurements in a partially cloudy field can have large fluctuations in measured photolysis frequencies. Radical species can rapidly respond to such fluctuations, but longer-lived species will not be in photochemical equilibrium, and will deviate from model predictions both positively and negatively. Because the destruction of some secondary species (such as CH2O, PAN, H2O2, and HNO3) provides chemical feedback into the modeled radical pool, over-prediction of these species by box models can have cascading effects on modeled rates of O3 formation. The broad suite of measurements and the diverse set of chemical and meteorological conditions sampled during KORUS-AQ provide a unique platform to evaluate model performance and evaluate the importance of observing these species to constrain O3 production estimates in a complex, heterogeneous megacity such as Seoul.
As noted in Section 3.2, model calculations were constrained by as many species as possible, including CH2O, PAN, H2O2, and HNO3 when measurements were available to allow for the most accurate representation of the feedback that these species provide. Although this set of highly-constrained calculations is expected to yield the most realistic estimates of radical abundances and rates of O3 production, much can be learned about model sensitivity and local chemistry by comparing results of highly-constrained model runs to those using fewer constraints. For this comparison, four additional set of model calculations were performed. All inputs were identical to those in the highly-constrained set of runs, except each set left one of the secondary species unconstrained: CH2O, PAN, H2O2, and HNO3. The following discussion examines the comparison between model calculations for each of these species with their observed values, the reasons for differences, and the significance of these differences to model estimates of net O3 production.
Figures 3, 4 and 5 examine observed versus calculated vertical profiles of H2O2, PAN, and CH2O for the descents of the DC-8 over Seoul. Each figure is separated into morning, midday, and afternoon, showing how observed and modeled vertical profiles evolve throughout the day. The top row of each figure shows the statistics of observed vertical profiles, the middle row shows the ratio of modeled/measured mixing ratios from “unconstrained” calculations, and the bottom row shows the calculated lifetimes of the given test species. The diurnal evolution of ambient H2O2 in the top panels of Figure 3 exhibits the combined influences of chemistry, deposition, and vertical mixing. In the morning, H2O2 was present in low amounts in the shallow boundary layer (median values below 200 pptv), while a reservoir of relatively high H2O2 (median values greater than 700 pptv) was present above 1 km. Here, we refer to the boundary layer as the lowermost region of the atmosphere that is directly impacted by surface emissions, which is typically very shallow (a few hundred meters) in the morning, and extends up to 1–2 km by the afternoon. The low mixing ratios of H2O2 in the morning boundary layer result from inhibited photochemical production of H2O2 as well as deposition throughout the night. Due to an overabundance of NOx, photochemistry in Seoul was radical-limited during KORUS-AQ (described in greater detail in Section 5), which limits chemical formation of H2O2 since reaction of HO2 with NO dominates over the HO2 self-reaction. This is exacerbated in the morning, when low photolysis, low vertical mixing, and strong NOx emissions would act to strengthen the radical-limited conditions. As the day progresses, mixing ratios of H2O2 at low altitudes increase, while mixing ratios aloft remain relatively constant. By the afternoon, there is little vertical gradient in H2O2; however, mixing ratios at lower altitudes never exceed those of the reservoir aloft. This behavior is consistent with H2O2 in the boundary layer over Seoul being largely driven by entrainment of air from the residual layer aloft. The vertical profiles of the ratio of modeled/measured H2O2 further support this hypothesis. Model/measured ratios of H2O2 at higher altitudes are closer to one than at low altitudes, indicating that the air in the residual layer is better described by the steady state assumption than air in the boundary layer. In the morning, for example, modeled/measured H2O2 ratios in the boundary layer were extremely low (below 0.1 at the lowest level), indicating model under-prediction of H2O2, while modeled/measured H2O2 ratios in the residual layer were typically between 0.5–1.5. The calculated lifetimes for H2O2 due to photochemical loss and deposition were on the order of 15–20 hrs and did not vary substantially with altitude. Comparatively, the H2O2 formation rates shown in Figure 3 exhibited large gradients with altitude and was driven primarily by the abundance of NO. As the day progressed, this led to underpredictions of H2O2 at higher altitudes as high NO values were mixed higher into the growing boundary layer. In effect, model calculations of H2O2 did not match measurements within the boundary layer because of the large variation in local formation rates versus the more dominant influence of vertical mixing (not accounted for in the model) delivering higher abundances of H2O2 produced aloft under conditions of much lower NO.
PAN, presented in Figure 4, exhibited small vertical gradients with higher mixing ratios tending toward lower altitudes. Values also increased throughout the day at all altitudes with afternoon values roughly double those observed in the morning. This behavior suggests that photochemical production from surface emissions drove the diurnal evolution of PAN observations. This is also consistent with the vertical gradient observed at midday when the boundary layer is still growing and the effect of surface emissions has yet to reach the top of the measured profile. Looking at modeled/measured mixing ratios, PAN was generally overestimated by the model, but the modest overestimates in the morning can be sharply contrasted with the large overestimates aloft later in the day. This model behavior can be best understood in the context of the PAN lifetime shown at the bottom of Figure 4. Model performance was best at the lowest altitudes where PAN lifetime was shortest and the expectation of steady-state the best. Nevertheless, the slight tendency to overestimate at these altitudes likely resulted from mixing of PAN from above where NOx was less abundant, but the lifetime of PAN was longer. The highest modeled/measured ratios occurred between 400–800 m in the morning, between 900–1,400 m at midday, and between 1,200–2,000 m in the afternoon. These altitudes roughly correspond to the range of boundary layer heights for those times of day. Those altitudes correspond to the longest PAN lifetimes in the profile that also have enough NOx to sustain a large PAN production rate. Also note that the largest discrepancies occur at the highest (coldest) altitudes only when sufficient NOx has mixed to those altitudes. As was the case for H2O2, these model discrepancies are ultimately caused by the vertical mixing that is not represented in the model. For PAN, it is the mixing from below that prevents the build-up of PAN to steady-state values at higher altitudes where PAN lifetimes are longer than the timescale for mixing. The widening of the range of modeled/measured PAN ratios at higher altitudes also reflects daily variability in the boundary layer height. For example, during Research Flight 7, the top of the boundary layer at midday was 1.5 km (as indicated by gradients in the test species and other short-lived species, such as NOx). During this time, the model/measured ratio increased with altitude before reaching a maximum value at 1.5 km, coincident with the top of the boundary layer. During Research Flight 10, on the other hand, the top of the boundary layer at midday was 1.3 km, and the maximum PAN modeled/measured ratio occurred at this height as well.
The vertical profiles of CH2O presented in Figure 5 also indicate photochemical production within the mixed layer. However, in contrast to PAN, model calculations of CH2O reasonably match observations at all altitudes and all times of day. One reason for this can be attributed to the much shorter calculated lifetimes for CH2O over Seoul which also had much less vertical variability than calculated PAN lifetimes; thus, the expectation for CH2O to approach steady-state is much greater for CH2O than either H2O2 or PAN. Because CH2O is closely related to the rate of VOC oxidation and the abundance of radical species (Wert, 2003; Parrish et al., 2012; Valin et al., 2015; Schroeder et al., 2016; Wolfe et al., 2016), model-measurement agreement indicates that the VOC mixture used to constrain the model and the underlying chemical mechanism are adequate to represent of ambient conditions for CH2O.
HNO3 (not shown) is another secondary species that was calculated in an unconstrained simulation. Modeled HNO3 consistently exceeded observations by greater than a factor of 10 within the boundary layer. This can be attributed in part to the lack of adequate sinks in the model, which did not account for uptake of HNO3 to form particulate nitrate.
Having shown that the steady-state assumption is inadequate for describing some species in Seoul, it is important to assess the associated feedbacks that these species have on modeled rates of net O3 production, P(O3), in Seoul. In addition to the previously-described sets of model calculations, an additional set simulations were run whereby all four test species were unconstrained. Comparison of these six sets of simulations (constrained, unconstrained, and the four simulations with each species unconstrained individually) allows for such an evaluation. Figure 6 shows cumulative distributions of calculated P(O3) from each of these model simulations. Between the constrained (black line) and unconstrained (gray line), there is a shift towards higher rates of P(O3) in the unconstrained runs. To understand this difference, these two sets of model runs are compared with those for each of the individually unconstrained species runs. A quick examination shows that the difference is entirely due to the constraint of PAN. This is due to the additional production of organic peroxy radicals resulting from the overpredicted PAN abundances in the unconstrained runs. The lack of model sensitivity to H2O2 and HNO3 is due to their weak roles as radical reservoirs in the polluted Seoul environment such that radical abundances and resulting rates of O3 production do not rely on their being well-represented in the model. Conversely, CH2O is a strong peroxy radical source, but it is generally well predicted by the model with model/measurement discrepancies that are evenly distributed around the observed values. Thus, differences in individual model runs between constrained and unconstrained calculations do not affect the overall distribution of P(O3). While it is difficult to quantify specifically, it is expected that the interpolation of hydrocarbon observations makes a large contribution to the discrepancies for individual model calculations while having no detectable impact on the aggregated statistics.
The exercises described above serve to highlight the importance of having a wide suite of measurements to constrain a box model in heavily polluted environments. In complex environments such as Seoul, where a confluence of strong time-varying local emissions, local meteorology, and background or residual pollution act to reduce the applicability of the steady-state assumption, the importance of model constraints is very high. In this case, without measurements of PAN to constrain the model, calculated rates of P(O3) in Seoul would be biased high by more than 40% when integrated over the distribution of calculated rates.
This bias related to overprediction of PAN is of particular concern given the intent to use the model to examine the sensitivity of P(O3) to changes in precursors. Such calculations must be conducted without constraining PAN as its abundance must be allowed to change along with precursors. While the reason for the PAN discrepancy is tied to the physical process of boundary layer mixing, it is necessary to represent this impact in the box model with a chemical analog. As noted earlier, the strong temperature dependence of PAN thermal decomposition leads to a large range of lifetimes for PAN (e.g., up to 10–15 hours near 2 km as shown in Figure 4). Such lifetimes are unrealistic, given the expectation of a much shorter time for vertical mixing in the boundary layer; thus, a first-order loss of PAN was introduced into the model that was based on thermal decomposition at the average temperature in the lowest 2 km during daily descents over Seoul. Given both daily and diurnal temperature changes, the average temperature was determined for each individual descent over Seoul to determine the first order loss rate to apply to each data point. This loss was calculated to be half the rate of thermal decomposition at the average temperature for the profile below 2 km. This first-order loss is artificial in that it represents nonlocal decomposition as air is vertically exchanged, acting to limit the buildup of PAN at higher altitudes where lifetimes were too long and also effecting minor reductions of PAN at lower altitudes where precursor abundances were much higher than other altitudes in the boundary layer profile. This procedure was applied not only to PAN, but also to other peroxyacyl nitrates in the model (e.g., PPN derived from alkanes, TPAN derived from aromatics, and MPAN derived from isoprene).
Conducting unconstrained model calculations with this additional loss term for peroxyacyl nitrates had a dramatic impact on model performance. The regression of model-calculated PAN against observations improved substantially, showing both a reduction in the bias and an improvement in the correlation between calculated and observed PAN. The PAN regression slope for Seoul decreased from 4.8 to 0.92, the intercept changed from –50 to –25, and the R2 increased from 0.33 to 0.49. The constrained calculations were also adjusted to include the new treatment of other peroxyacyl nitrates (PPN, TPAN, and MPAN), resulting in an 11% reduction in the integrated ozone production shown in Figure 6. Most importantly, the bias in ozone production between constrained and unconstrained calculations was dramatically reduced with integrated ozone production for the unconstrained calculations being only 8% lower than the constrained calculations. This modification to the model as applied to KORUS-AQ conditions allows for a more confident analysis of ozone production sensitivity to precursors, which is pursued in subsequent sections.
A final point of comparison is obtained by comparing calculated rates of net O3 production to observed changes in O3. For this comparison, results from the constrained set of model runs (with updated treatment of peroxyacyl nitrates) are examined for the repeated profiling by the DC-8 over Seoul during the descents over Olympic Park which consistently sampled the same ground track from an altitude of 1 km down to a few tens of meters above the surface.
Table 3 shows statistics for average Ox, O3, and model-calculated P(O3) from the morning, midday, and afternoon descents over Seoul. From the morning to midday, an average change of 17 ppbv of Ox (16 ppbv of O3) over a period of 3.5 hours yields an observed rate of change of Ox (and O3) of ~4.8 ppbv/hr, compared to the average calculated P(O3) between morning and midday of 5.6 ppbv/hr. Likewise, from midday to afternoon, the observed change of 16 ppbv of Ox (20 ppbv of O3) over a period of ~3.5 hours yields an observed rate of change of Ox of ~4.6 ppbv/hr (and ~5.7 ppbv/hr for O3) compared to the average calculated P(O3) between midday and afternoon of 7.8 ppbv/hr.
|Profile Time||Average Ox (O3) [ppbv]||Average P(O3) [ppbv/hr]||Average local time|
These aggregate statistics demonstrate the strong role of photochemistry in the O3 changes observed over Seoul. It is also important, however, to recognize that other influences on O3 such as advection, entrainment from above, and surface deposition are not represented in the box model. Each of these factors should reduce O3 on average since Seoul is a strong source region and may explain the higher calculated rates of production as compared to observed changes.
Understanding O3 sensitivity, that is, whether local O3 production is NOx-limited or radical-limited (VOC-limited), is a critical step towards drafting effective mitigation policies. During KORUS-AQ, DC-8 flights took advantage of natural gradients in O3 and its precursors by repeatedly overflying Seoul and Taehwa forest, located ~30 km to the southeast, on many different days and under different conditions. A summary of these DC-8 observations for altitudes below 1 km is shown in Figure 7, contrasting data from the overflight of the two sites in the morning, midday, and afternoon. The most noticeable difference is that NOx mixing ratios were always lower over Taehwa than over Seoul at all times of day with median values that were 2-6 times lower over Taehwa, Seoul also exhibited a much wider range of extreme values, especially in the morning when emissions were concentrated near the surface before substantial boundary layer growth had occurred. NOx levels were lower outside the city due to dilution of the primary emissions as they moved downwind, as well as chemical processing. By contrast, CH2O, an excellent proxy for VOC chemistry, was very similar between the two sites (with the exception of Taehwa in the morning), and roughly constant throughout the day. This is consistent with the continuous oxidation of VOCs and the short lifetime of CH2O. The lower morning CH2O at Taehwa also suggest a role for biogenic VOC emissions which increase throughout the day with temperature. O3 and Ox increased steadily from morning to afternoon at both sites, consistent with a photochemical source. While Ox distributions were similar, O3 tended to be higher over Taehwa in relation to Seoul due to the partitioning between O3 and NO2 under the high NOx conditions in Seoul. The bottom left panel in Figure 7 shows net O3 production rates calculated from the constrained set of model runs. Compared to the observed quantities, P(O3) behaves most like CH2O, as both map closely to photochemistry with lower morning values versus midday and afternoon. The lack of change in P(O3) across the large NOx gradient demonstrates the NOx-saturated behavior in the model calculations. This allows sustained ozone production to increase both O3 and Ox across the region throughout the day. Thus, these observations provide a natural experiment whereby O3 production is sustained over a large NOx gradient, without an associated gradient in VOCs (based on the CH2O proxy), demonstrating that O3 production across the SMA was radical-limited (i.e. VOC-limited or NOx-saturated). This builds upon recent work by Kim et al., (2018), who used measurements from an instrumented ground site in Seoul to identify conditions as radical-limited, by using airborne measurements throughout the boundary layer over a large area to understand O3 sensitivity over the broader SMA.
The findings highlighted in the previous section indicate that effective O3 mitigation strategies in the SMA must include reductions in VOC emissions. However, because VOCs as a class contain a broad spectrum of different species with a wide range of reactivities and radical yields, exploring the contributions of individual VOCs or classes of VOCs to the overall rate of O3 production is a crucial next step towards identifying emissions sectors that contribute disproportionately to O3 production. To better understand the sensitivity of O3 to specific VOC classes, additional box model simulations were conducted whereby select VOC constraints were set to zero in the model. For these simulations, the model was not constrained by observations of CH2O, PAN, HNO3, and H2O2 because of the associated feedback that removal of VOCs would have on these species. Figure 8 shows the distribution of calculated O3 production rates over Seoul using a complete suite of DC-8 observations (black dashed line) compared to simulations where a single hydrocarbon or group of hydrocarbons were removed from the model (orange line in each panel). Note that because of the complex feedback that VOCs have on radical abundances and HOx/NOx partitioning, the percent reductions shown in Figure 8 do not add up to 100%. The general shape of the P(O3) distribution in the black dashed line (i.e. base-case) shows two distinct modes: one centered around 0–1 ppbv/hr and one centered around 4–5 ppbv/hr. In general, the lower mode contains data collected in the morning, at higher altitudes (1–2 km), and features low concentrations of NOx (mean 0.3 ppbv) and low concentrations of short-lived hydrocarbons (for example, a median isoprene concentration of 0). The data that make up this mode are characterized as clean or aged airmasses above the boundary layer that were not recently impacted by surface emissions. The second mode, centered around 4–5 ppbv/hr, features data that contain characteristics of urban pollution, with relatively high NOx (mean 11 ppbv) and VOCs.
C7+ Aromatic compounds (which include toluene, ethylbenzenes, and xylenes) are shown to have the greatest impact on modeled O3 production, with a 32% reduction in mean P(O3) and a sharp change in the distribution, with a large reduction in the amount of data falling above 5 ppbv/hr. Modeled O3 production was also fairly sensitive to isoprene, with removal of isoprene yielding a 15% reduction in mean P(O3) over Seoul. Alkenes (which include ethene, propene, C4 alkenes, and C5 alkenes) also were found to contribute an important amount to O3 production in Seoul, with removal of alkenes resulting in a 14% reduction in mean P(O3). In contrast to C7+ Aromatics, removal of either isoprene or alkenes from the model resulted in little change in the modeled distribution of P(O3) above 5 ppbv/hr. In effect, removing C7+ Aromatics from the model had a large effect on points with very high values of P(O3), while removing isoprene or alkenes tended to mostly impact points that were producing below 5 ppbv/hr in the base-case simulation. Other VOCs, including light alkanes, heavy alkanes, methanol, and CO (not shown) had negligible effect on modeled P(O3). Figure 8 shows results of sensitivity simulations over Seoul, but similar results were noted when the study area was expanded to the entire SMA: Removal of C7+ Aromatics yielded a 36% reduction in mean P(O3), isoprene a 13% reduction, alkenes a 13% reduction, and all other species yielded 7% or less. Additionally, the results shown in Figure 8 include all data collected below 2 km, which may mask the contribution of very short-lived VOCs, like isoprene, which have vertical profiles that are weighted towards the surface. When data are filtered to only include data collected below 1 km over Seoul, the percent reductions in mean P(O3) become 34% (C7+ Aromatics), 16% (isoprene), 13% (alkenes), 3% (C4+ alkanes), 1% (light alkanes), and 6% (methanol). Thus, no matter how the data are filtered (Seoul only, whole SMA, low altitudes only, etc.), the results suggest that reductions in anthropogenic emissions, particularly C7+ Aromatics (and alkenes, to a lesser extent), could provide an attractive target for reductions in local O3 production. This finding will benefit from source apportionment work being conducted by other KORUS-AQ investigators to characterize sources and quantify emissions of these species in the SMA. By contrast, the natural source of isoprene from vegetation does not offer an effective target for emissions reduction but must be considered to understand the response of O3 chemistry to emissions reductions for anthropogenic VOCs.
While reductions in C7+ aromatics would benefit local O3 production in Seoul, the regional extent of downwind production must also be considered. The higher levels of O3 and P(O3) at Taehwa (see Figure 7), despite the lower concentrations of NOx, highlights the regional impact that the very high NOx in Seoul has on sustaining O3 production downwind and across the surrounding region. Thus, despite the large gradient in NOx from inside Seoul and into the surrounding region shown in Figure 7, conditions remain conducive to high rates of O3 production over a very large area and the only way to limit the regional extent of ozone production is to also target NOx emissions for reduction.
In a strongly radical-limited environment, initial reductions in NOx for a given VOC abundance will result in an increase in P(O3). After a sufficient amount of NOx is removed, modeled P(O3) will reach a maximum at the point where O3 sensitivity transitions to a NOx-limited environment. Further reductions in NOx beyond this point result in decreases in P(O3) relative to the maximum, though P(O3) may still be higher than at the starting point. To assess the impact of NOx reductions, model sensitivity to NOx was evaluated using three additional simulations whereby model input values for NO were reduced by 25%, 50%, and 75% while all other inputs were kept the same. Two additional simulations were performed where NOx and all relatively-short-lived anthropogenic VOCs (i.e. all VOCs except methane, CO, and isoprene) were reduced by 10% and 25%. Table 4 shows the mean relative increase in modeled P(O3) from these experiments, filtered to show data from the entire SMA, Seoul, and non-Seoul SMA below 2 km. Over the entire SMA, reducing model input NO by 25% yielded a mean relative increase in modeled P(O3) by 5%, becoming 11% when NO was reduced by 50%. Upon reducing input NO by 75%, P(O3) was still higher than the base simulation by 10% on average, but was slightly lower than the simulations where NO was reduced by 50%. This indicates that, aggregated over the entire SMA, O3 sensitivity changed from radical-limited to NOx-limited over this experimental range of NO reductions. In simulations where both NOx and VOCs were reduced, mean P(O3) decreased relative to the base simulation, demonstrating the value in concurrent reduction in emissions for both.
|Mean Relative Change in Modeled P(O3)|
|Model Simulation||All SMA <2 km||Seoul <2 km||non-Seoul SMA <2 km|
|NO + VOC –10%||–1%||–2%||–2%|
|NO + VOC –25%||–3%||–6%||–6%|
When only data from urban Seoul are considered, reductions in NO always lead to an increase in P(O3), with the percent increase becoming higher with each subsequent NO reduction. This indicates that even with a 75% reduction in NO, the photochemical environment in urban Seoul is largely radical-limited. Interestingly, the changes in P(O3) from urban Seoul suggest that it is substantially more radical-limited than the SMA taken as a whole. Because of this, suppression of radicals (and P(O3)) in urban Seoul leads to a lower base-case P(O3) compared to the entire SMA, and therefore a larger relative increase in P(O3) as the photochemical environment approaches the transition point where O3 production is most efficient When only non-Seoul data were considered, the calculated mean relative increases in modeled P(O3) with NO reductions were lower than the other two datasets (i.e. all SMA and urban Seoul), and the mean relative change in P(O3) finally goes negative with the –75% simulation. As such, the “starting point” in the base-case simulation for non-Seoul was closer to the photochemical transition point than all SMA or urban Seoul.
These observations, combined with the results presented in Section 5.1, might suggest that reductions in VOC emissions should be a sole priority for reducing O3 in the SMA, and that reductions in NOx emissions would exacerbate the problem. While reducing NOx in our simulations resulted in increases in modeled P(O3) in all but one case, it is also important to consider the associated feedbacks on key O3 precursors, particularly NOx itself. Because NOx has a lifetime on the order of hours, ambient NOx mixing ratios are the result of a balance between NOx emissions and NOx removal. While reductions in NOx emissions would certainly lead to reductions in ambient NOx mixing ratios, we must also consider how the lifetime of NOx changes in response to associated changes in the photochemical environment. Table 5 shows weighted averages of instantaneous NOx lifetimes as calculated by our model, assuming that formation of HNO3 is the only NOx removal process. Reductions in constraining NO resulted in generally lower NOx lifetimes compared to the base-case simulation, with the –75% simulation in urban Seoul yielding the largest reduction: a 66% decrease in the NOx lifetime relative to the base-case simulation. This is important for two reasons: 1) Reduction in NOx emissions will result in amplified reductions in ambient NOx mixing ratios (for example, a 25% reduction in NOx emissions should be expected to produce ambient NOx reductions in excess of 25%, all else being equal, because of associated reduction in the NOx lifetime), and 2) A shorter duration of O3 production as airmasses move downwind from urban Seoul. While select VOCs, such as isoprene, are very short-lived, the majority of VOCs that were abundant in Seoul have lifetimes that are longer than NOx, including aromatics (toluene, for example, has a lifetime of 1–2 days). In an environment such as the SMA, where VOCs are dominated by aromatics and emissions of biogenic VOCs persist throughout the region, the duration of O3 production for a given polluted airmass as it moves downwind is essentially limited by the lifetime of NOx in that airmass. Therefore, even though reductions in NO resulted in increased rates of O3 production throughout the SMA in our simulations, the regional extent of O3 production would be reduced. In Figure 7, we showed that a receptor site at Taehwa Forest consistently had lower NOx mixing ratios than urban Seoul. If NOx mixing ratios in urban Seoul were reduced by some amount, NOx mixing ratios at receptor sites such as Taewha would be expected to be reduced by a larger amount, since a higher percent of NOx would be chemically removed while in transit (owing to the shorter NOx lifetime). In effect, while reductions in NOx emissions could result in locally higher rates of O3 production in urban Seoul, regions outside of urban Seoul should benefit if the associated NOx reductions push them far enough into the NOx-limited regime. Fully quantifying the effects of NOx reductions on O3 throughout the SMA requires the use of 3D models that can account for emissions, transport, and chemistry, and is beyond the scope of this work, but this question is being pursued by other KORUS-AQ investigators (Oak et al., 2019).
|weighted average of τNOx (hrs), weighted by F(O3)|
|Simulation||All SMA <2 km||Seoul <2 km||non-Seoul SMA <2 km|
As South Korea has experienced rapid industrial growth over the past few decades, exposure to unhealthy levels of O3 has emerged as a public health concern, particularly in the SMA (population 25 million). Data collected by a network of ground stations in the SMA during KORUS-AQ indicated that O3 exceed the Korean 8-hour AQS value on 39 days during the 41-day study period. Furthermore, O3 was observed to be highest in outlying suburban regions, particularly Gyeonggi province, rather than urban Seoul. In this work, airborne observations of O3 and other trace gases were used alongside an observationally-constrained 0-D photochemical box model to explore the sensitivity of O3 to changes in its precursors. The fidelity of these photochemical calculations was explored using a series of additional simulations, and it was found that the steady state assumption used in 0-D box models cannot describe select intermediate species, particularly PAN, H2O2, and HNO3, while ambient CH2O observations were well-represented by our model. Model shortcomings in the prediction of H2O2 and HNO3 had no impact on model-calculated rates of O3 production, while model results not constrained by PAN observations overpredicted average O3 production in Seoul by more than 40%. This was mitigated by introducing a first order loss for PAN and other thermally labile peroxyacyl nitrates based on the average temperature in the boundary layer profiles of Seoul, providing much better agreement between constrained and unconstrained calculations of O3 production. When fully constrained, aggregate statistics for model-predicted rates of O3 production agreed well with average observed changes in ambient O3.
Observed gradients in O3 and its precursors between urban Seoul and a downwind receptor site (Taehwa Forest) indicated that O3 production in the SMA was radical-limited (i.e. VOC-limited) over the study period. Additional zero-out simulations were performed whereby select VOCs were removed from the model, allowing for diagnosis of model sensitivity to individual VOCs. These simulations identified C7+ aromatics (i.e. toluene, xylenes, ethylbenzenes, etc.) as the dominant VOC contributor to O3 production in the region, with a 32% reduction in mean O3 production calculated when C7+ aromatics were removed from the model. Isoprene was found to be the second most important VOC with respect to contribution to O3 production (15% reduction in mean O3 production), and anthropogenic alkenes were the third most important (14% reduction in mean O3 production).
Though the SMA was identified as radical-limited, analysis of model simulations in which NOx was reduced provided insight on competing effects. When constraining NO was reduced by up to 75% in our model, O3 production increased in Seoul but began to decrease for the surrounding area. Thus, areas outside of Seoul were found to transition from a radical-limited to a NOx-limited environment within the range of NOx reductions studied here, while urban Seoul remained radical-limited even at a 75% reduction in constraining NO. Furthermore, we found that in all regions of the SMA, reductions in constraining NO lead to decreases in the modeled NOx lifetime. The results of a shortened NOx lifetime could be two-fold: 1) as the plume from urban Seoul moves downwind towards receptor sites, the time-duration over which that plume is capable of producing high amounts of O3 would be shortened, and 2) reductions in NOx emissions should be accompanied by reductions in the NOx lifetime, meaning that for a given reduction in NOx emissions, a larger decrease in ambient NOx mixing ratios could be expected. These results indicate that, even though the SMA was identified as radical-limited, reductions in NOx emissions would have complex effects on O3 in the SMA, whereby O3 in urban Seoul would likely increase as a result of reduced NOx emissions, but regions outside of urban Seoul, particularly Gyeonggi province, could benefit. Additional benefits of NOx reductions include reductions in ambient NO2 (which is a criteria pollutant itself), and potential for reductions in fine particulate matter. However, analysis of these co-benefits is beyond the scope of this work.
The policy implications of this work are clear: reductions in VOCs, particularly C7+ aromatic compounds, provide an effective pathway for reducing O3 production in the SMA. Anthropogenic alkenes, such as ethylene and propylene, also provide an attractive target for emissions reductions, but certainly should not be prioritized over C7+ aromatics. Isoprene, while an important contributor to O3 production, does not represent a viable target for emissions reductions, owing to the biogenic nature of its source. The KORUS-AQ dataset can be utilized to classify and quantify sources of VOCs in the SMA, which may provide fruitful information for policymakers in drafting targeted mitigation strategies aimed at specific emissions sectors. Although O3 production in the SMA is radical-limited, reductions in NOx emissions should also be considered with the intent of reducing the regional extent of O3 production. Broad-scale measurements of VOCs and NOx in the SMA must be continued to understand changes in source contributions throughout the year, and to understand the effectiveness of any policies that are implemented. Long-term ground-based studies could provide continuous measurements at discrete locations, and follow-up airborne studies could be leveraged to explore emissions trends and gradients over larger spatial scales. While the O3 sensitivity analysis provided in this work and other studies that analyze in-situ measurements from KORUS-AQ can point to specific emissions sources that would make for attractive targets for emissions reductions, fully understanding the effects of emissions reductions on future air quality requires the use of 3D models that implement emissions, transport, and chemistry. Because of this, it is imperative that the emissions parameterizations used in 3D models are realistic, and the measurements from KORUS-AQ can provide an attractive dataset to test and validate 3D models. Additional studies that compare the chemical mechanisms used in 3D models and other models (such as the LaRC box model used in this study) may also highlight potential strengths or shortcomings of the underlying chemical mechanisms used in 3D models. If veracity can be obtained for modeled emissions and chemistry, a larger degree of confidence in the outcomes of simulations with different emissions reductions scenarios can be gained.
Outputs from all box model simulations used in this work are available on the KORUS-AQ archive: https://www-air.larc.nasa.gov/cgi-bin/ArcView/korusaq?MODEL=1.
The KORUS-AQ study was jointly funded by NASA and the Korean National Institute of Environmental Research (NIER). Special thanks goes to all who made the DC-8 flights over Seoul and in Korean airspace possible. This includes civil and military air traffic coordinators, DC-8 pilots and crew, and the scientists who negotiated the flight paths and permissions needed to collect these observations. The members of the PTR-MS instrument team (P. Eichler, L. Kaser, M. Müller) are acknowledged for their support with instrument preparation and field work.
PTR-ToF-MS measurements aboard the NASA DC-8 during KORUS-AQ were supported by the Austrian Federal Ministry for Transport, Innovation and Technology (bmvit) through the Austrian Space Applications Programme (ASAP) of the Austrian Research Promotion Agency (FFG).
The authors have no competing interests to declare.
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