Changes in anthropogenic precursor emissions drive shifts in the ozone seasonal cycle throughout the northern midlatitude troposphere
- 1Physics Department, Carleton College, Northfield, MN, USA
- 2Met Office Hadley Centre, Exeter, UK
- 3University of Leeds Met Office Strategic (LUMOS) Research Group, School of Earth and Environment, University of Leeds, Leeds, UK
- 4NASA Goddard Institute for Space Studies, New York, NY, USA
- 5Center for Climate Systems Research, Columbia University, New York, NY, USA
- 6Meteorological Research Institute, Tsukuba, Japan
- 7NOAA Geophysical Fluid Dynamics Laboratory, Princeton, NJ, USA
- 8Beijing Climate Center, China Meteorological Administration, Beijing, China
- 9Hohenpeissenberg Meteorological Observatory, Deutscher Wetterdienst, Hohenpeissenberg, Germany
- 10David.D.Parrish LLC, Boulder, CO, USA
Correspondence: Henry Bowman (firstname.lastname@example.org) and David D. Parrish (email@example.com)
Simulations by six Coupled Model Intercomparison Project Phase 6 (CMIP6) Earth system models indicate that the seasonal cycle of baseline tropospheric ozone at northern midlatitudes has been shifting since the mid-20th century. Beginning in ∼ 1940, the magnitude of the seasonal cycle increased by ∼10 ppb (measured from seasonal minimum to maximum), and the seasonal maximum shifted to later in the year by about 3 weeks. This shift maximized in the mid-1980s, followed by a reversal – the seasonal cycle decreased in amplitude and the maximum shifted back to earlier in the year. Similar changes are seen in measurements collected from the 1970s to the present. The timing of the seasonal cycle changes is generally concurrent with the rise and fall of anthropogenic emissions that followed industrialization and the subsequent implementation of air quality emission controls. A quantitative comparison of the temporal changes in the ozone seasonal cycle at sites in both Europe and North America with the temporal changes in ozone precursor emissions across the northern midlatitudes found a high degree of similarity between these two temporal patterns. We hypothesize that changing precursor emissions are responsible for the shift in the ozone seasonal cycle; this is supported by the absence of such seasonal shifts in southern midlatitudes where anthropogenic emissions are much smaller. We also suggest a mechanism by which changing emissions drive the changing seasonal cycle: increasing emissions of NOx allow summertime photochemical production of ozone to become more important than ozone transported from the stratosphere, and increasing volatile organic compounds (VOCs) lead to progressively greater photochemical ozone production in the summer months, thereby increasing the amplitude of the seasonal ozone cycle. Decreasing emissions of both precursor classes then reverse these changes. The quantitative parameter values that characterize the seasonal shifts provide useful benchmarks for evaluating model simulations, both against observations and between models.
Tropospheric ozone is a harmful air pollutant and greenhouse gas. It is a secondary pollutant, formed as a photochemical product of oxidation reactions involving volatile organic compounds (VOCs), carbon monoxide (CO) and methane (CH4) in the presence of oxides of nitrogen (NOx). Entrainment of stratospheric ozone also contributes to tropospheric ozone concentrations. Ozone is lost from the troposphere to surface deposition and additional photochemical reactions. The processes driving ozone formation and destruction are complex, which adds difficulty to the task of understanding the impacts of tropospheric ozone on human and ecosystem health and climate change. Because ozone is not directly emitted, areas of ozone formation and enhanced concentrations are often geographically separated from emission sources. The lifetime of ozone in the troposphere is long enough – approximately 22 d averaged globally (Young et al., 2013) – that it is transported over hemispheric scales. Its lifetime is even longer above the planetary boundary layer (PBL) due to slower losses in the free troposphere (FT) and continuing formation from transported precursors (Fowler et al., 2008). At northern midlatitudes (defined here as between 30 and 60∘ N), prevailing westerly winds and the long lifetime of ozone result in a high degree of zonal similarity in baseline ozone concentrations (Chan et al., 2010; Parrish et al., 2014), with similar temporal changes in baseline ozone observed at multiple sites throughout that zone (Cooper et al., 2014; Parrish et al., 2020). In this work, we use the term “baseline” to denote air that has not been influenced by direct, recent continental influences – see discussion in chap. 1 of Hemispheric Transport of Air Pollution 2010 (HTAP, 2010). Another consequence of rapid transport of ozone and its precursors is that emissions from any location in the northern midlatitude region can influence ozone concentrations throughout the zone. Depending on emissions upwind of a particular site, that site may be representative of only baseline ozone conditions or of a combination of baseline conditions and regional or local processes.
At northern midlatitudes, outside of the marine boundary layer (MBL), tropospheric ozone follows a seasonal cycle with annual maximum concentrations in late spring or early summer, due to peak stratospheric influence in late winter or spring; peak photochemical production in the summer (e.g., Logan et al., 1985); and a summertime emission maximum of the important biogenic VOC precursors (e.g., Guenther et al., 1995). Within the MBL, ozone has a summertime minimum due to the much faster photochemical ozone losses in that season and the absence of strong photochemical production due to limited NOx emissions in that environment. However, the seasonal ozone cycle has not been constant over time; many previous studies have noted a shift in the seasonal ozone cycle. These studies have been measurement- and model-based, cover northern midlatitude locations in Europe and North America, and describe shifts in either the amplitude or phase of the seasonal ozone cycle. For example, a seasonal cycle shift at Hohenpeissenberg, Germany, has been identified, based on observations, in which ozone reached its annual maximum in the summer in the 1970s, but now ozone is nearly equal between the spring and summer seasons (Parrish et al., 2012, 2013). Other studies have found similar shifts in the timing of the annual ozone maximum at other European sites (Parrish et al., 2012; Cooper et al., 2014, and references therein), the eastern USA (Bloomer et al., 2010), California (Cooper et al., 2014; Parrish et al., 2017) and the western USA (Cooper et al., 2012). Other papers have indirectly provided evidence of a shift in the phase of the seasonal ozone cycle without expressly mentioning this shift. For example, studies have documented increasing springtime ozone (Lin et al., 2015), often in combination with decreasing summer ozone (Chan et al., 2010; Cooper et al., 2012; Lin et al., 2017), which indicates that the seasonal cycle is shifting towards a springtime maximum.
Some studies discuss another aspect of the varying seasonal ozone cycle: changes in its amplitude. This finding is most evident in measured data collected across the USA (Simon et al., 2014), specifically in the eastern USA (Strode et al., 2015). Other studies do not explicitly mention the changing amplitude but still provide evidence for this phenomenon. According to measurements and models, these papers find ozone decreasing in summer, when it has typically been highest (Hogrefe et al., 2011; Cooper et al., 2012; Parrish et al., 2012, 2013, and references therein; Simon et al., 2014; Lin et al., 2017), and concurrently increasing in the winter, when it has typically been lowest (Bloomer et al., 2010; Chan et al., 2010; Cooper et al., 2012; Parrish et al., 2012; Lin et al., 2017). In combination, these changes imply that the amplitude of the seasonal ozone cycle has decreased from its level in the 1990s, which was a time period characterized by decreasing precursor emission concentrations across northern midlatitudes.
Ozone precursor emission changes have been hypothesized as the cause of shifts in the seasonal ozone cycle in some studies, which have reached a consensus about how emissions affect the seasonal cycle. In the absence of large anthropogenic precursor emissions, the seasonal ozone maximum occurs in the spring (Logan et al., 1985; Cooper et al., 2014, and references therein). Higher emissions correspond to a seasonal cycle of larger magnitude with seasonal maximum ozone occurring later in the year (in summer); likewise, lower emissions correspond to a seasonal cycle of smaller amplitude with a spring maximum that occurs earlier in the year (Parrish et al., 2013; Clifton et al., 2014; Cooper et al., 2014; Strode et al., 2015). Most of these studies investigate areas affected only by baseline conditions or areas where local emissions have been controlled in recent years; thus, they capture the decrease in amplitude and shift towards an earlier maximum. However, there is some analysis of areas with increasing emissions, and the seasonal cycle grew in amplitude with a progressively later maximum. For example, NOx emissions have roughly tripled since 1990 in parts of China, and summertime ozone has increased at many polluted sites (e.g., sites directly downwind of these increasing emissions) by up to 2 ppb yr−1 (Li et al., 2020); thus, on local to regional scales in China, increasing emissions correspond to a growing seasonal cycle with a shift towards summer. Most of the European and North American studies have largely been based on observations and simulations from the late 20th century and early 21st century, when emissions were generally decreasing. One exemption is the study of Marenco et al. (1994), who noted that the preindustrial 19th century seasonal maximum occurred in the spring at a remote European site, but that maximum had shifted towards the summer by the 1980s. Taken together, these results suggest that the increase in anthropogenic precursor emissions during industrial development shifts the ozone seasonal cycle toward the summer, and reductions in those emissions allow the seasonal cycle to shift back toward the preindustrial condition.
Other studies identify correlations between precursor emissions and a changing seasonal cycle at sites separated geographically (instead of at the same site studied across a period of time). For example, sites in eastern Canada are subject to less pollution than sites in the eastern USA and subsequently show smaller summertime and larger wintertime ozone concentrations, evidence that the amplitude of the seasonal cycle is smaller in the absence of precursor emissions (Chan et al., 2010). Across the same sites, a springtime ozone maximum is observed for more pristine Canadian sites, while the more polluted eastern USA displays a summertime maximum (Chan et al., 2009). Similarly, Clifton et al. (2014) note that the polluted northeastern region of the USA displays a summertime seasonal ozone maximum, whereas the more pristine intermountain western region displays a springtime seasonal maximum.
A quantitative understanding of the link between precursor emissions and the seasonal ozone cycle will benefit air quality policy development. Rieder et al. (2018) note that changes in the seasonal ozone cycle may influence the timing and number of days of ozone exceedance above the US National Ambient Air Quality Standards (NAAQS). As such, understanding the seasonal cycle – including how it changes in response to changing emissions – may usefully inform air quality control managers across the world in setting future ozone standards in efforts to reduce the harmful impacts of surface ozone (Lin et al., 2017). A changing future climate will bring further uncertainty, including the possibility of an ozone–climate penalty in which rising temperatures can offset tropospheric ozone reductions from precursor emission control (Rasmussen et al., 2013; Clifton et al., 2014; Jaidan et al., 2018). Moreover, Schnell et al. (2016) report that a warming climate may cause changes to the seasonal cycle of tropospheric ozone independent from seasonal cycle effects of changing emissions. Jaidan et al. (2018) and Rieder et al. (2018) describe the possibility of a similar “methane penalty” in which rising methane concentrations offset the reduction of other ozone precursors. Under some modeled scenarios, a future reversal of the present-day seasonal ozone cycle may be possible due to ozone precursor emission reductions in combination with the ozone–climate penalty (Clifton et al., 2014). We can reduce some of this uncertainty by understanding the interactions between emissions and atmospheric impacts (e.g., the seasonal ozone cycle) as fully as possible.
Despite the extensively documented record of shifts in the seasonal ozone cycle, no previous study has quantitatively analyzed measured data and model simulation results from across the northern midlatitude region, examined shifts in the amplitude and phase of the seasonal ozone cycle, quantitatively analyzed changing precursor emissions alongside seasonal cycle shifts, and proposed the mechanisms by which changing emissions affect the seasonal cycle; this paper aims to accomplish these tasks. We examine sites representative of baseline conditions in both western Europe and North America. Given the zonal similarity of ozone at northern midlatitudes, our analysis is expected to be representative of the baseline troposphere throughout northern midlatitudes. We investigate seasonal ozone cycle changes that began ∼75 years ago, before reliable ozone measurements are available; thus, we rely on historical simulations from the Coupled Model Intercomparison Project Phase 6 (CMIP6) Earth system models (ESMs) as our primary basis for seasonal ozone cycle analysis. We compare these simulation results to available observations. A previous study of seasonal ozone cycle found that the previous generation of Earth system models poorly simulated the seasonal cycle, including changes to it (Parrish et al., 2013). However, Griffiths et al. (2021) find that CMIP6 ESMs capture the general shape of the observed seasonal ozone cycle averaged between 30 and 90∘ N, despite a positive bias of 3–4 ppb in overall ozone concentrations. Thus, CMIP6 ESMs may be more reliable for ozone seasonal cycle analysis than previous models.
In this work, we investigate two quantities that define the seasonal cycle of tropospheric ozone: the amplitude (the difference between the annual average and the annual maximum or minimum ozone concentrations) and the phase (the timing of annual maximum ozone concentrations). Model simulations indicate that both of these quantities have changed over past decades; we compare their shifts with temporal changes in ozone precursor emissions that are prescribed in the models. In the following sections, we describe our analytical methods, present the analysis results and discuss those results within a broader context. The overall goal of the paper is to provide a quantitative analysis of the shifting seasonal cycle of tropospheric ozone at northern midlatitudes. As the seasonal cycle reflects the sources and loss of ozone, quantifying it provides the opportunity for comparison of the simulated seasonal cycle between different models as well as for comparison of model simulations with the limited record of observations. Comparing models and observations is an important way to gain insight into the performance of the models.
In this work, we seek to quantify the ozone seasonal cycle based on a small set of parameter values that reflect the amplitude and phase of that cycle. To accomplish this quantification, we analyze monthly mean ozone concentrations from ESM simulations as well as observations, to the extent they are available. Monthly means have sufficient temporal resolution to capture seasonal changes, while effectively averaging over most variability driven by diurnal and meteorological changes. Our goal is to investigate the long-term changes in the seasonal cycle over the period included in the CMIP6 historical simulations (Eyring et al., 2016), which were designed to extend from 1850 to the near present, which was set as 2014. Ozone varies systematically on decadal scales, and it also has temporal variability on interannual scales (i.e., on the scale of a few years) driven by changes in large-scale transport patterns in the troposphere. For our purposes, this sub-decadal variability is “noise”; we minimize the obscuring effects of this variability by selecting analysis techniques that effectively average over this variability.
2.1 Model simulation results
Time series of monthly mean ozone concentrations simulated by the CMIP6 ESMs are our primary basis for investigating changes in the seasonal ozone cycle; an example time series is shown in Fig. 1. These ozone time series come from six different models: BCC-ESM1, CESM2-WACCM, GFDL-ESM4, GISS-E2-1-H, MRI-ESM2-0 and UKESM1-0-LL. Table S2 in the Supplement gives references for descriptions of these ESMs and their model output. Results of CMIP6 model simulations are archived at the Earth System Grid Federation (https://esgf-node.llnl.gov/projects/cmip6/, last access: 10 September 2020) and are freely available to download. We obtained monthly mean ozone concentrations for all six ESMs at the model levels that correspond to the selected comparison locations. Where available, a mean of multi-ensemble members was calculated for each model from the CMIP6 historical simulations over the period from 1850 to 2014.
2.2 Fit equations
We fit time series of monthly mean ozone concentrations with the following equation, which has separate functions for the average long-term change (LTC) and the superimposed seasonal cycle (SC):
where t is time in years. We find representing LTC(t) by a five-term power series (i.e., a five-term polynomial),
captures the long-term changes and allows detrending of the monthly means for quantification of the seasonal cycle. The choice of five polynomial terms in the power series is arbitrary: a range of polynomial terms (2 to 12) successfully detrends the monthly means without affecting seasonal cycle parameter values; Sect. S1 in the Supplement gives further details.
Quantification of the seasonal cycle is complicated by significant shifts in both the amplitude and phase of the seasonal cycle over the last ∼75 years of the time series, as illustrated in Fig. 1. Annual maximum ozone moved from primarily March and April (pink, purple or blue) before 1900 to primarily June (blue-green and light green) by the 1980s, while the vertical spread of the time series increased from ∼12 ppb before 1900 to ∼20 ppb by 1980. SC(t) must capture both the preindustrial seasonal cycle and the seasonal cycle shifts beginning around 1940. A two-term Fourier series quantifies the preindustrial seasonal cycle (PISC) in the detrended monthly means:
where A1 and φ1 are the respective amplitude and phase of the fundamental (one sine cycle per year), and A2 and φ2 are the respective amplitude and phase of the second harmonic (two sine cycles per year) of the Fourier series. As discussed in Sect. S2 in the Supplement, the fundamental is generally larger in magnitude than the second harmonic; together, these two harmonics capture nearly all variance associated with the seasonal cycle, so higher order harmonics are not quantified.
Inclusion of two Gaussian functions separately capture the shifts in the magnitude and phase of the seasonal cycle; these are added to the A1 and φ1 parameters in of Eq. (3) to quantify changes in the amplitude and phase of the fundamental harmonic without affecting the A1 and φ1 parameter values:
Equation (4) quantifies both the PISC(t) and the later shift in the seasonal cycle. The r and rφ parameters represent the magnitude of the Gaussian functions, the m and mφ parameters represent the time of their maximum values, and the s and sφ parameters represent their widths. Gaussian functions are only included in the fundamental term because it is the only harmonic to consistently shift across locations and models. Note that the A1 and φ1 parameters characterize the amplitude and phase of the preindustrial seasonal cycle in Eq. (4), as the Gaussian maxima contribute negligibly before ∼1900. Thus, the sums (A1+r) and (φ1+rφ) derived here are most appropriate to compare to the A1 and φ1 values derived from a similar equation without the Gaussian terms (e.g., in Parrish et al., 2019), as earlier work analyzed observations collected only in the last few decades.
Substitution of Eqs. (2) and (4) into Eq. (1) gives Eq. (5):
In the following, analysis ozone time series are fit to this equation, which consistently captures more than 95 % of the variance in the time series of monthly mean ozone. In these fits, the derived parameter values are more precisely fit if the time origin is chosen within the time series span. Here, we choose the year 2000 (i.e., t= year − 2000); Parrish et al. (2019) fully discuss the implications of this choice.
We fit time series of the annual ozone precursor emissions (PE) that are prescribed in the models from anthropogenic and biomass burning sources with an equation similar to Eq. (1); it has separate terms for the preindustrial long-term change (PITC) and more complex behavior (EG) during industrial development:
A linear function,
quantifies the early long-term change in average precursor emissions. The EG term of Eq. (6) is given by a Gaussian function that is consistent with an increase and then decrease in emissions primarily driven by anthropogenic activity:
This term is analogous to the Gaussian functions included in Eqs. (4) and (5); rem represents the maximum, mem represents the year of that maximum and sem represents its width. Substitution of Eqs. (7) and (8) into Eq. (6) gives Eq. (9):
which captures more than 98 % of the variance in the precursor emission time series.
Fitting of ozone and precursor emission time series with these similar equations allows for quantitative comparison between the ozone seasonal cycle shift and the growth and decrease in emissions. Specifically, comparison of the ozone seasonal cycle Gaussian parameters in Eqs. (4) and (5) with the precursor emission parameters in Eqs. (8) and (9) is the basis for examining the correlation between changes in the seasonal cycle and changing ozone precursor emissions.
The multivariate regression fits of Eqs. (5) and (9) to time series of monthly mean ozone concentrations and annual emissions, respectively, quantify confidence limits for all derived parameter values. In this work, 95 % confidence limits are tabulated and discussed throughout. However, these confidence limits only reflect the variability in the time series about the functional form fit to that time series, and this approach assumes that each member of the time series is an independent variable with no autocorrelation within the time series; hence, it must be recognized that these confidence limits are lower estimates of the actual uncertainties of the derived parameter values.
2.3 Selected CMIP6 simulation locations
The CMIP6 ESMs provide monthly mean ozone concentrations on global grids. To focus our investigation on northern midlatitudes, model-simulated monthly mean ozone time series are taken from model cells at three locations in western Europe and three locations in western North America. The European locations are surface sites at Hohenpeissenberg, Germany, and Jungfraujoch, Switzerland, and in the FT above Jungfraujoch at altitudes between 5 and 6 km. The North American locations are situated in California – one surface site in the USA, in Lassen Volcanic National Park (hereafter Lassen Volcanic NP), and two sites in the FT above Trinidad Head at two different altitudes: between 0.9 and 1.2 km in different models (we refer to this site as Trinidad Head at 1 km for simplicity) and between 5 and 6 km. Table 1a summarizes the model-simulated location details, including the surface site elevations. In some cases, the model cells containing surface sites were not the lowest model cell; instead, model cells with the average elevation closest to actual site level were chosen. For example, cell altitudes varied between 3.2 and 3.8 km for Jungfraujoch.
These six evaluation locations were chosen for three key reasons. First, there are measurement records at these locations spanning from 2 to nearly 5 decades, which allows for the quantification of the observed seasonal cycle and comparison between models and measurements. Second, the sites chosen on both continents have somewhat similar environments. Sites on both continents are in the western continental regions, which allows transported baseline ozone to dominate the ozone concentrations. Each continent includes a location in the FT between 5 and 6 km, an elevated surface site (Jungfraujoch and Lassen Volcanic NP), and a location situated at or near the 1 km elevation (Hohenpeissenberg and the FT above Trinidad Head at 1 km). The lowest-elevation sites are a surface site in Europe and a sampling of the troposphere at 1 km altitude over North America, so there is not exact correspondence in site selection between the two continents. Finally, the sites chosen are representative of multiple different environments: low-, medium- and high-altitude site locations in both Europe and North America. The sites on each continent are all within ∼500 km; given the pronounced zonal similarity of ozone concentrations at midlatitudes (Parrish et al., 2020), the geographic separation between these sites has negligible impact on ozone concentrations, so the two sets of three sites are representative of their respective continents at different altitudes or elevations. In summary, the locations are selected to provide an altitude-dependent contrast between the western regions of the two continents.
a Although sonde measurements were not conducted above Jungfraujoch, we analyzed model simulation results above Jungfraujoch for comparison with the European FT measured data set (see Table 1b). b An offshore location selected for comparison with onshore and is only considered in the Supplement. Details included in Sect. S4 in the Supplement. c Sonde measurements from Hohenpeissenberg, Uccle and Payerne are averaged to form the European FT data set; more detail is given in Sect. 2.4. d Surface measurements from Jungfraujoch, Zugspitze and Sonnblick are averaged to form the European alpine data set; more detail is given in Sect. 2.4.
2.4 Ozone observations
Although model simulations are our main basis for analysis, observational data are also considered. Shifts in the amplitude and phase of the seasonal ozone cycle are generally apparent in observational records that span long enough time periods. The measurements serve to check the accuracy of model simulations; realistic model simulations are expected to at least approximately reproduce the observed seasonal cycle and its temporal shifts.
Our analysis includes three observational data sets from both Europe and North America. The European data sets include one spanning 47 years (1971–2017) at Hohenpeissenberg, Germany; one spanning 40 years (1978–2017) averaged between three European alpine sites (Jungfraujoch, Switzerland; Zugspitze, Germany; and Sonnblick, Austria); and one spanning 20 years (1998–2017) averaged between measurements from sondes launched from European sites at Hohenpeissenberg (Germany), Uccle (Belgium) and Payerne (Switzerland). We consider average sonde measurements between 5 and 6 km. The impetus behind averaging measurements from three surface sites and three sonde data sets is to reduce the impact of ozone variability in any one data set, thereby obtaining a more precise quantification of ozone over western Europe. These same data sets have been considered in previous studies of western European baseline ozone concentrations (Parrish et al., 2014, 2020). The Hohenpeissenberg data discussed by Parrish et al. (2014) are extended through 2016 here, and the European alpine and sonde data sets are the same as those analyzed by Parrish et al. (2020). The North American data sets include one spanning 30 years (1998–2017) at Lassen Volcanic NP and one spanning ∼21 years (late 1997–early 2018) from sondes launched from Trinidad Head. We consider average sonde measurements between 5 and 6 km and between 0.5 and 1.0 km. These North American data sets are also the same as those analyzed by Parrish et al. (2020). Table 1b summarizes location details of observational data considered in the analysis.
2.5 Precursor emissions
Annual mean ozone precursor emissions were derived from ESM emission inventories integrated over the northern midlatitude region between 30 and 60∘ N for the 1850–2014 simulation period. The primary analysis examines emissions of NOx and VOCs from anthropogenic (Hoesly et al., 2018) and biomass burning sources (van Marle et al., 2017) that were provided as a common emission inventory to be used by all models (including the six in this study) in CMIP6 simulations. As discussed in further detail in Sect. S5 in the Supplement, the anthropogenic emissions dominate this inventory. Although there are small seasonal cycles in these emissions, these seasonal cycles are either approximately constant over the entire time interval or their relative magnitudes are small compared with that of the seasonal cycle of ozone; further discussion is included in Sect. S5.
Even though the six ESMs used the same prescribed anthropogenic and biomass burning emissions, Fig. 1 of Griffiths et al. (2021) shows that subtle differences remain in NOx emissions and even greater differences remain in CO and biogenic VOC emissions between models. Differences in the VOC emissions arise because the speciated VOC emissions that were provided had to be mapped onto the chemical mechanisms in the individual models, and this mapping may not fully account for the total VOC emissions prescribed. The emissions that are the focus of our analysis have been taken from the prescribed emission inventory; we have not further diagnosed the exact northern midlatitude emissions actually used in each individual model.
Some of the models were able to provide quantifications of emissions from biogenic and other natural sources for evaluation. These emissions varied between models based on model-specific chemistry and parameterizations, and they included biogenic VOC emissions (specifically, isoprene) and dimethyl sulfide (DMS) from oceans as well as NOx emissions from soil and lightning. Methane is considered independently due to its very long lifetime compared with other VOCs; all of the ESMs use prescribed global annual mean values of CH4 concentrations as input at the surface throughout the whole historical period (Meinshausen et al., 2017). Further details of model-specific natural emissions and CH4 are given in Sect. S6 in the Supplement.
3.1 Isolating the seasonal cycle: detrending monthly means and harmonic analysis
Ozone in the troposphere varies on a wide spectrum of temporal scales, which makes it difficult to quantify a particular contribution to that variability. To isolate the seasonal cycle, we examine time series of monthly mean ozone concentrations. Monthly means integrate over the short-term variability driven by diurnal cycles and short-term meteorological changes, which effectively removes their influence. The time series considered here span a maximum of 165 years, which allows significant influence from “longer-term” (i.e., on the scale of decades to centuries) variations driven by ozone precursor emission changes and climate variations. We isolate the seasonal cycle from these longer-term changes by detrending the monthly mean concentrations, which we accomplish by subtracting LTC(t) in Eq. (1) from the time series of monthly means. A regression fit of the five-term polynomial given in Eq. (2) to the time series of monthly means gives values for the five polynomial coefficients; Sect. S1 discusses the determination of LTC(t) in more detail. Figure 2 shows the example time series of Fig. 1 with the fit to Eq. (2) indicated by the black curve, which quantifies the longer-term temporal change that underlies the time series of monthly means. Figure 2 also includes a fit to the complete Eq. (5), shown in red. The seasonal cycle of the detrended monthly means is apparent as variation in the monthly means (blue dots) about the black curve. As expected, the detrended monthly means display an annually repeating seasonal cycle.
Any repeating signal, such as the seasonal ozone cycle, can be quantified by a linear combination of sinusoidal functions (i.e., a Fourier series). The seasonal cycles that we examine are described sufficiently by the sum of the first two harmonics: the fundamental (one sine cycle per year) and the second harmonic (two sine cycles per year) as indicated in Eq. (3). The fundamental is generally larger in magnitude than the second harmonic, except for the two lower-elevation North American sites, for which the two harmonics were approximately equal in magnitude during the preindustrial period. In combination, the fundamental and second harmonic capture almost all the variance associated with the seasonal cycle. A quantitative Fourier analysis that provides the basis for this harmonic analysis and the inclusion of only the first two harmonics is detailed in Sect. S2. The detrended seasonal cycles, including their evolution over the course of the 1850–2014 period, are analyzed for the six ESM simulations at the six selected northern midlatitude locations; this is the primary basis of our analysis, which is discussed in the next three subsections.
3.2 Model-simulated preindustrial seasonal cycle
To understand the magnitude and timing of changes to the seasonal ozone cycle that began near the middle of the 20th century, it is important to quantify the seasonal cycle before those changes began (i.e., the preindustrial seasonal cycle). Only very limited ozone measurements are available before the mid-20th century, so our quantitative analysis of the preindustrial seasonal cycle is limited to model simulations. Fits of Eq. (3) to the time series of detrended monthly means quantify the contributions of the fundamental and second harmonic; detailed descriptions of similar fits to time series of monthly means from observations in the MBL and FT are given by Parrish et al. (2016) and Parrish et al. (2020), respectively. Each fit provides four parameter values that quantify the preindustrial seasonal cycle for a model simulation at a particular location. Figure 3 quantitatively examines the simulated preindustrial seasonal cycle in the FT between 5 and 6 km at locations above Europe and North America. Because these are higher-altitude locations, they are more physically separated from ground-based sources of emissions than are surface sites. We assume that these locations are representative of the FT baseline seasonal ozone cycle with little influence from local or regional emissions; thus, they are appropriate for our initial analysis. At both FT locations, the preindustrial seasonal cycle is similar in character; it is determined largely by the fundamental, which generally reaches its seasonal maximum in May or June. Figures S4 and S5 in the Supplement give plots similar to Fig. 3 for the four lower-elevation locations, with discussion in Sect. S3 in the Supplement.
Between different models, there are important qualitative similarities in the simulated preindustrial seasonal cycle at most locations. First, the fundamental is larger in magnitude than higher-order frequencies, except for Trinidad Head at 1 km and Lassen NP. Second, the maximum of the fundamental occurs in the late spring or early summer, which drives an overall seasonal maximum that also occurs in the late spring or early summer. Marenco et al. (1994) report a similar seasonal cycle with a springtime maximum based on late-19th century observations at Pic du Midi, a remote mountaintop site in France; given the paucity of measurements from the preindustrial period, this is the strongest comparison available between measurements and model simulations.
Despite qualitative similarities, there are quantitative differences in simulations among models at specific sites and within individual model results across different sites. Figure 3 indicates that the amplitudes of the simulated seasonal cycles vary by a factor of ∼3. Exclusion of the GISS-E2-1-H model, which Griffiths et al. (2021) note simulates the strongest response of tropospheric ozone to precursor emissions of CMIP6 models, lowers this factor to ∼2. Additionally, the models do not all reproduce the degree of zonal similarity of the seasonal cycle at northern midlatitudes noted by Parrish et al. (2020); the amplitude and phase of both harmonics and the overall seasonal cycle differ significantly between the European and North American FT sites in some model simulations. These patterns are also present at the other, lower-elevation locations examined (Figs. S4, S5).
3.3 Seasonal cycle shifts across northern midlatitudes
Across all models and all locations, shifts in both the amplitude and phase of the seasonal cycle are ubiquitous. Importantly, the presence of a seasonal cycle shift in the FT indicates it is a hemisphere-wide phenomenon, rather than limited to a localized environment. Figure 4 compares preindustrial and modern-day seasonal cycle simulations from one example model with the observed modern-day seasonal cycle in the FT over Europe. This is the same example time series shown in Figs. 1–3. The modern-day seasonal cycle is larger in amplitude with a later maximum compared with the preindustrial seasonal cycle. These changes are primarily driven by the changing fundamental, rather than the second harmonic, which makes only a small contribution in the FT and is not statistically different between the preindustrial and modern-day simulations. The modern-day simulated seasonal cycle approximates but does not exactly match observations from the past 2 decades; the simulated seasonal cycle is smaller in amplitude with an earlier maximum than the measured seasonal cycle.
The temporal evolution of the fundamental harmonic for all model simulations and measurements is shown in Figs. 5 and 6 for all six locations. The colored curves in these figures are derived from the fits of Eq. (5) to the respective time series of simulated monthly means; they represent the evolution of the amplitude (left panels) and phase (right panels) of the fundamental over the period of the simulations. In general, in each simulation, the fundamental is approximately constant in magnitude and phase for roughly the first half of the time series, depending on the model and site, before significant shifts begin. Most of the models agree that the amplitude began to increase and the phase began to change near the middle of the 20th century, so that the seasonal maximum appeared later in the year compared with the preindustrial values. Near the end of the 20th century, these changes began to reverse. The Gaussian functions incorporated in Eqs. (4) and (5) are generally defined precisely in the model simulation fits. However, fits to some simulated time series return no statistically significant parameters for the corresponding Gaussian function, and the resulting curve in Fig. 5 or 6 is then a horizontal line; the MRI-ESM2-0 simulation at both FT locations is such an example. Such horizontal lines indicate either that the model simulated a constant fundamental amplitude/ phase (i.e., no shift in that harmonic property) or that the variability in the simulated monthly means was too large to allow a statistically significant measure of the shift in the fundamental phase or amplitude to be discerned.
The fits of Eq. (5) to the measured time series (black curves) are much less certain than the fits to the model simulations due to the much shorter period of the measurements, which also generally exhibit greater variability. In all of the measured time series from the FT and at some surface sites, only the average of the amplitude and phase of the fundamental over the measurement period can be extracted from the available data; in Figs. 5 and 6, these averages are indicated by horizontal line segments that span that measurement period. The two longest measurement records were collected at the two European surface sites; Fig. 5 shows the shifts in the seasonal cycle extracted from these records. In North America, only the seasonal cycle phase at Lassen Volcanic NP (Fig. 6e) shows a significant shift; however, that shift can only be quantified by a linear one-parameter function (equal to the slope) replacing the Gaussian three-parameter function in Eq. (5). This fit is indicated by the sloping line segment in the figure that spans the measurement period. This line segment does approximate the shape of the Gaussian fits to two of the corresponding model simulations. It should also be noted that the linear fit to the phase shift is closely related to an earlier analysis approach (Parrish et al., 2013) that also quantified the phase shifts from observations at some of these same sites. Table 2 compares the present results with those earlier ones. Overall, the results agree within their confidence limits at Hohenpeissenberg, the European alpine sites (Jungfraujoch and Zugspitze analyzed separately in the earlier work) and Lassen Volcanic NP. At the European sites, the present results do indicate smaller slopes, which is consistent with their inclusion of data from more recent years when the shift in the phase of the seasonal cycle slowed.
3.4 Connection between ozone precursor emissions and the seasonal cycle
All six CMIP6 ESM simulations incorporated the same ozone precursor emission inventory for anthropogenic and biomass burning sources. Figure 7a illustrates the temporal evolution of these non-methane VOC and NOx emissions integrated annually and over the entire northern midlatitude region (30 to 60∘ N). The curves in Fig. 7b are fits of Eq. (9) to those emissions; these fits (with the underlying linear increases) capture more than 98 % of the variance in the time series of annual emissions. Equation (9) is designed to provide Gaussian function fits to the emissions, so that the derived parameters can be directly compared to the Gaussian parameters that quantify the shift in the ozone seasonal cycle. Figures S10 and S11 in the Supplement compare the Gaussian parameters from the emission fits with those derived from fits to the model simulated ozone at individual sites.
The parameters from individual model simulations exhibit large variability between the six locations, particularly at lower elevations. To more precisely compare the seasonal cycle shifts with the temporal evolution of the emissions, we average the Gaussian parameters in various ways over sites and model simulations. We average over all three model-simulated European locations, all three North American locations, the three higher-elevation locations (the FT above Trinidad Head and Jungfraujoch between 5 and 6 km, and the European alpine sites), the three lower-elevation sites (Hohenpeissenberg, Lassen Volcanic NP and the troposphere above Trinidad Head at 1 km), each model simulation at all six sites, and an overall average over all six simulations at all six locations.
Figure 8 compares these averages with the Gaussian parameters from the emission fits and the limited measurement results; these averages are also included in Figs. S10 and S11. Table 3 and Table S3 in the Supplement list some of these model simulation averages, along with the ozone precursor emission and measurement parameters. The averaging of parameters across different selections of simulations and locations minimizes the influence of localized emissions and any site-specific behavior. All of these results are weighted averages, where each parameter value from an individual simulation result is weighted by the inverse of the square of the confidence limit of that parameter. In Fig. 8, the parameters derived at the six locations by the individual models are omitted for clarity; Figs. S10 and S11 show those same graphs with the individual model/location parameters included with their confidence limits. These figures serve to collect the results of the analyses, and they provide the basis for discussion of these results in the following section.
Interpretation of the confidence limits quoted for the derived parameters is difficult. The multivariate regressions utilized to fit the model simulations, observations and emissions return parameter values with 95 % confidence limits, which are plotted in Figs. 3, 4 and 8; many are not visible because they are smaller than the plotted symbols. These confidence limits are underestimated (see Sect. 2.2) due to autocorrelation in the time series of monthly mean ozone concentrations. An independent estimate of the confidence limit of each overall average parameter value can be obtained from the variance of the individual parameter values included in the average. If one assumes that each seasonal shift parameter must be identical at all six locations and that each model simulation at each site provides an independent determination of that parameter value, the confidence limit of the average can be estimated from the square root of the variance divided by the number of independent model determinations (36 if the fits to each of the six model simulations returns a parameter value at each of six locations). Such upper limits are included in parentheses in the bottom line of Table 3 and are included as the blue error bars on the overall averages in Fig. 8; they are larger by factors of 2.5–17 compared with those derived from the weighted averages of the parameters from the regression fits. In quantitative comparisons of the parameters from observations and emissions with those simulated, this issue with the confidence limits must be considered.
We analyze the seasonal cycle of tropospheric ozone over the historical period, as simulated by six CMIP6 Earth system models and deduced from available observations at six northern midlatitude locations in western Europe and western North America. Over the time period of the model simulations (1850–2014), the seasonal cycles shifted significantly in both phase and amplitude at all locations, including within the free troposphere. The seasonal cycles simulated by the models remained generally constant from 1850 until well into the 20th century; this preindustrial seasonal cycle is shown in Fig. 3 for two FT locations and in Figs. S4 and S5 for four lower-elevation locations. In the period from approximately 1920 to 1940, the seasonal cycle amplitude began to increase, and the seasonal maximum began to shift to later in the year. These changes reached their maximum extent late in the 20th century, after which they began to reverse – the seasonal cycle decreased in amplitude and the annual maximum shifted back to earlier in the year. Gaussian functional fits quantify these shifts. Observations are available for at most only the last 44 years of the model simulations; within their large uncertainties (see error bars in Fig. 8), the available measurements indicate seasonal cycle shifts similar to those simulated. Figure 4 illustrates these shifts as simulated by one model at one location; it shows that the fundamental harmonic is the primary contributor to both the seasonal cycle and its shifts. Figure 4 also compares the simulated modern-day seasonal cycle with that derived from observations. Figures 5 and 6 show comparisons of the shifting amplitude and phase of the fundamental harmonic among all models and with available observations at the six locations considered. Section 1 discussed extensive literature reports of modeled and observed changes in the seasonal ozone cycle throughout northern midlatitudes over the most recent 3 to 4 decades; the seasonal cycle shifts examined here are generally consistent with those reports.
Throughout northern midlatitudes, on average (blue symbols in Fig. 8) the simulated shifts in both the amplitude and phase of the fundamental of the seasonal cycle maximize at similar times (∼1985; Fig. 8a, b), with the amplitude shift having a somewhat smaller width (∼30 years; Fig. 8c) than the phase shift (∼40 years; Fig. 8d). At the maxima, the fundamental amplitude (Fig. 8e) had increased by ∼5.5 ppb (i.e., a ∼11 ppb increase in the difference between the seasonal minimum and maximum), and the seasonal maximum (Fig. 8f) had shifted to ∼3 weeks later in the year. For comparison, the average simulated preindustrial seasonal cycle in the free troposphere had an amplitude of ∼7 ppb and a seasonal peak near 1 June (Figs. 5, 6). The sparse measurement record from the European alpine sites and Hohenpeissenberg (respective red and green points in Fig. 8; entries in Table 3) agrees well with respect to the timing of the maximum shifts, but it suggests somewhat smaller seasonal cycle changes in the widths and magnitudes of those shifts; however, the large uncertainty in the observational determinations should be noted.
The model simulations exhibit large variability, both among models and locations (compare points on right side of graphs in Figs. 8, S10 and S11); however, it is difficult to judge if this variability is statistically significant. Here, we identify some aspects of this variability that appear to be robust. First, the relative spread among the model averages in the phase shift is greater than that in the amplitude for all three parameters (year of maximum as well as the width and magnitude of the Gaussians quantifying the shifts). Second, both the amplitude and phase shifts appear larger and more varied at lower elevations compared with the FT (compare lower graphs in Figs. 5 and 6 with the FT results in the upper graphs, and the low- and high-elevation averages in Figs. 8e and f and S12 in the Supplement); as the anthropogenic emissions are located at the surface, this behavior may reflect the greater influence from local and regional emissions at the surface sites compared with the more isolated locations in the FT. Third, Hohenpeissenberg (located at a relatively low elevation in central western Europe) generally shows the largest amplitude shifts in the model simulations as well as in the measurements, although the measurement results are highly uncertain. At Hohenpeissenberg (Fig. 5c), all six models simulated the timing of the maximum amplitude shift (i.e., the m parameter) within the uncertainty of that derived from the measurements (1987±6 years). This temporal agreement occurs despite disagreement (by a factor of ∼2) in the maximum fundamental amplitude (peaks of Gaussian curves in the Fig. 5c) and disagreement (up to a factor of ∼3) by two of the six models in the amplitude of the preindustrial fundamental (horizontal portion of the curves on the left of Fig. 5c). There is poorer agreement regarding the phase shift at Hohenpeissenberg, with the simulated maxima occurring between 1984 and 2000 in the six model simulations; the timing of the maximum phase shift derived from the measurements is not precisely defined, but its confidence limits include (nearly) all of the model results. Fourth, the greatest variability in the simulated phase shifts is seen at Trinidad Head at 1 km (Fig. 6f), which is the lowest-elevation North American location considered here; there, the maximum of the fundamental is found to occur in nearly every month of the year over the simulation period in at least one of the model simulations, although the seasonal cycle amplitude is relatively small at this location, which makes determination of that maximum difficult. A possible explanation for these divergent model results is that this location is on the edge of two transitions – the MBL to FT and the marine to continental environment – which may be a particularly difficult situation for the models, which have coarse horizontal resolution, to simulate.
We also quantify the temporal changes in total northern midlatitude ozone precursor emissions from anthropogenic and biomass burning sources (Fig. 7) that are incorporated into the emission inventories assumed by all of the ESMs. Between 1850 and 1940, emissions increased only slowly, with more rapid increases beginning in the mid-20th century as the result of rapid industrialization in Europe and North America. By the late 20th century, emissions began to decrease as the result of air quality control efforts in more developed countries. Notably, the changing emissions are driven by anthropogenic activity; Sect. S5 compares the temporal changes in anthropogenic and biomass burning emissions and shows that it is only the anthropogenic emissions that rise and fall over time, whereas the biomass burning emissions remain approximately constant.
On average, the parameters that quantify the shifts in the seasonal cycle correlate strongly with those that quantify the emissions. Figure 8a–d show that the overall model simulation averages of the four parameters that quantify the timing of the shift in the amplitude and phase of the fundamental harmonic closely correspond to the parameters that quantify the temporal evolution of the emissions. There is significant variability in the results from the different models (open circles on the right in the graphs in Fig. 8), but that variability is reduced in four regional averages (open circles on the left). There is no consistent, strong difference between the European and North American continents. Both the amplitude and phase shifts apparently maximized earlier in North America than Europe, but there is a great deal of variability among the individual determinations (Figs. S10, S11), so the statistical significance of this apparent difference is uncertain. There may also be significant differences in the shapes of the Gaussian describing the phase shift between the lower-elevation surface sites (i.e., earlier years of maximum shift and greater widths) compared with the higher-elevation sites representative of the FT (Fig. 8b, d); and the phase shift at high elevations appears to have maximized later with a smaller width. The maxima of the amplitude and phase shifts (Figs. 8e and f and S11) are apparently larger at the low-elevation sites, which may reflect more direct impact by anthropogenic emissions.
Based on the temporal correlation between the emission changes and the seasonal cycle shifts shown in Fig. 8, we hypothesize that changing ozone precursor emissions are the cause of the shifts in the seasonal ozone cycle throughout northern midlatitudes. During industrial development, ozone production driven by rising anthropogenic precursor emissions progressively becomes the predominant source of ozone, which shifts the ozone seasonal maximum into the summer, when photochemical ozone production is more important (compared with, e.g., ozone input from stratospheric intrusions, which peaks in the spring). Ozone production driven by anthropogenic activity also increases the amplitude of the seasonal cycle by boosting summertime concentrations while wintertime concentrations are less affected. As emissions decrease, those changes reverse, with the seasonal cycle returning toward the preindustrial cycle. Although ozone precursor emissions from all sources influence ozone production and the ozone seasonal cycle, it is anthropogenic activity that drives the seasonal cycle changes; more discussion of natural and anthropogenic emissions is given Sects. S5 and S6 and Figs. S7–S9 in the Supplement. The temporal correlation between the changes in emissions and the ozone seasonal cycle does not necessarily prove our hypothesis, but a comparison of ozone seasonal cycles between the southern and northern midlatitudes does support a causal relationship. As discussed and illustrated in Sect. S7 in the Supplement, we find no evidence of a significant shift in the phase nor the magnitude of the ozone seasonal cycle at southern midlatitudes. The presence of a shift in the ozone seasonal cycle throughout northern midlatitudes and its absence at southern midlatitudes is as expected from our hypothesis, due to the much smaller anthropogenic ozone precursor emissions in the Southern Hemisphere. For reference, Fig. 8 of Crippa et al. (2020) illustrates the dramatic difference in emissions from fossil fuel combustion between hemispheres.
An interesting aspect of the correlation between precursor emissions and the ozone seasonal cycle shifts is the temporal offset in the evolution of the emissions. The Gaussian function fit to the non-methane VOC emissions in Fig. 7 (see Table S3a for parameter values) peaked in ∼1983 with a full width at half maximum (FWHM, which is a factor of 1.67 larger than the Gaussian s parameter) of ∼47 years, whereas the fit to the NOx emissions peaked in ∼1995 with a FWHM of ∼63 years. The shifts in the amplitude and the phase of the average simulated ozone seasonal cycle both reached peaks in ∼1985, closely corresponding to the VOC emission peak. The FWHM of the ozone seasonal cycle amplitude shift (∼48 years) also closely matches the FWHM of the VOC emissions. In contrast, the FWHM of the ozone seasonal cycle phase shift (∼65 years) corresponds more closely to the FWHM of the NOx emissions. A simple hypothesis can provide a qualitative explanation for this correspondence. The VOC emissions provide fuel for the photochemical production of ozone; thus, these emissions exert primary control on the seasonal cycle amplitude driven by summertime production. The NOx emissions provide the catalyst that determines whether photochemistry produces or destroys ozone – once the NOx emissions are large enough that photochemical production dominates the seasonal cycle and moves the seasonal maximum into the summer, the phase shift ends, as the maximum cannot continue shifting into the autumn, and the seasonal maximum will not shift back until NOx emissions decrease to levels low enough that photochemical production no longer dominates the ozone budget. In summary, we are suggesting that the NOx emissions largely control the timing of the seasonal maximum in ozone, whereas the VOC emissions control the seasonal cycle amplitude. If this hypothesis is correct, consideration of the role of biogenic VOCs could help to explain some of the diversity in the seasonal cycles and shifts seen among the model simulations; as can be seen in Fig. 1 of Griffiths et al. (2021), the temporal variation in the biogenic VOC emissions are significantly different across the models.
Assuming that the above hypotheses are correct, the ozone seasonal cycle shift derived from observations must reflect the time evolution of emissions, thereby providing tests of the emission estimates upon which the model simulations are based. The measurement records (maximum of 44 years) are so short that the precision of the parameters of the seasonal cycle shift that can be derived from the measurements (see Table 3) is limited, as indicated by the relatively large confidence limits for those parameters included in Fig. 8. However, two points can be noted. First, the average year of the maximum shift in the amplitude of the observed ozone seasonal cycle (1990±3 years) is later than the maximum of the VOC emissions (1983±1 year); as we expect these two maxima to be the same, this disagreement may indicate that anthropogenic VOC emissions actually peaked a few years later than indicated in the emission inventory. The uncertainty in the year of the maximum phase shift determined from observations (1985±8 years) prevents a precise comparison between the emission maxima and the phase shift maxima. Second, the widths of the amplitude and phase shifts in the observed seasonal cycle (15±9 and 17±17 years, respectively) appear to be smaller than the widths of the NOx and VOC emissions (38±2 and 28±2 years, respectively).
The seasonal cycle of ozone reflects the annual variability in the sources and sinks of ozone; thus, its accurate simulation is expected to present a stringent test for models. Given the paucity of the observational ozone record (both spatially and, more importantly, temporally), improved confidence in our understanding of changes in the seasonal ozone cycle must primarily come from improved agreement between different model simulations. Our analysis has focused on changes in anthropogenic and biomass burning emissions, which were prescribed from the same source to the extent possible for all models; however, there were differences in the implementation of the prescribed emissions into the models, mainly from VOCs due to the individual requirements of the chemistry scheme within each model. In addition, the representation of natural emissions (e.g., biogenic VOCs emitted from vegetation) differed between individual models, giving variation in the natural to anthropogenic emission ratios between models. Thus, the remaining differences in emissions between models may cause some of the inter-model variation. More generally, Griffiths et al. (2021) suggest that differences in the simulation of ozone from CMIP6 models could be due to inter-model variations in the treatment of chemical and physical processes, including dynamic transport, stratosphere–troposphere exchange, photolysis, deposition, convection and boundary-layer schemes. There is a need to go beyond direct model–observation comparison studies; for example, multi-model perturbed parameter ensembles can be used to intercompare the sensitivity of models to different input parameters and/or parameterizations (Wild et al., 2020). Notably, in this work, we document relatively large seasonal cycle shifts that are common to the entire northern midlatitude baseline troposphere; given the magnitude of these shifts, which we attribute to changing precursor emissions, it may be difficult to independently determine the effects of other factors, e.g., changing climate (Fowler et al., 2008; Clifton et al., 2014), on the northern midlatitude ozone seasonal cycle.
All of the data utilized in this paper are available from public archives; most are fully discussed and referenced in the Acknowledgments section of Parrish et al. (2020, https://doi.org/10.1029/2019JD031908). One additional data set is included in this paper, the surface observations at Hohenpeissenberg, which is available from the Tropospheric Ozone Assessment Report database (https://toar-data.org, Schultz et al., 2017).
The supplement related to this article is available online at: https://doi.org/10.5194/acp-22-3507-2022-supplement.
HB and DDP designed the research and performed the analysis; SEB, KT, MD, NO, FMO, LH, TW and JZ performed model simulations; ST extracted model simulation results; DK provided the Hohenpeissenberg measurement data; HB and DDP wrote the paper with input from all co-authors.
David D. Parrish works as an atmospheric chemistry consultant (David.D.Parrish, LLC); he has had contracts funded by several state and federal agencies and an industrial coalition, although they did not support the work reported in this paper.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Henry Bowman's efforts were supported by Carleton College's endowed internship funds, in particular by the Littell Internship Fund, designed to support undergraduate student internships with a focus on environmental studies. Steven Turnock would like to acknowledge support from the UK-China Research and Innovation Partnership Fund through the Met Office Climate Science for Service Partnership China (CSSP China) as part of the Newton Fund. Fiona M. O'Connor would like to acknowledge support from the BEIS and DEFRA Met Office Hadley Centre Climate Programme (grant no. GA01101). Makoto Deushi and Naga Oshima were supported by the Japan Society for the Promotion of Science KAKENHI (grant nos. JP18H03363, JP18H05292, JP19K12312 and JP20K04070), the Environment Research and Technology Development Fund (grant nos. JPMEERF20202003 and JPMEERF20205001) of the Environmental Restoration and Conservation Agency of Japan, the Arctic Challenge for Sustainability II (ArCS II; program grant no. JPMXD1420318865), and a grant for the Global Environmental Research Coordination System from the Ministry of the Environment, Japan (grant no. MLIT1753). Susanne E. Bauer and Kostas Tsigaridis acknowledge support (in the form of resources) from the NASA High-End Computing (HEC) Program through the NASA Center for Climate Simulation (NCCS) at Goddard Space Flight Center. The CESM project is supported primarily by the National Science Foundation. Computing and data storage resources, including the Cheyenne supercomputer (https://doi.org/10.5065/D6RX99HX), were provided by the Computational and Information Systems Laboratory (CISL) at NCAR. NCAR is sponsored by the National Science Foundation. The authors are grateful to the Earth System Grid Federation (https://esgf.llnl.gov, last access: 10 September 2020) for archiving the CMIP6 model simulation results and making them available to the scientific community.
This paper was edited by Frank Dentener and reviewed by two anonymous referees.
Bloomer, B. J., Vinnikov, K. Y., and Dickerson, R. R.: Changes in seasonal and diurnal cycles of ozone and temperature in the eastern U. S., Atmos. Environ., 44, 2543–2551, https://doi.org/10.1016/j.atmosenv.2010.04.031, 2010.
Chan, E.: Regional ground-level ozone trends in the context of meteorological influences across Canada and the eastern United States from 1997 to 2006, J. Geophys. Res., 114, D05301, https://doi.org/10.1029/2008JD010090, 2009.
Chan, E. and Vet, R. J.: Baseline levels and trends of ground level ozone in Canada and the United States, Atmos. Chem. Phys., 10, 8629–8647, https://doi.org/10.5194/acp-10-8629-2010, 2010.
Clifton, O. E., Fiore, A. M., Correa, G., Horowitz, L. W., and Naik, V.: Twenty-first century reversal of the surface ozone seasonal cycle over the northeastern United States, Geophys. Res. Lett., 41, 7343–7350, https://doi.org/10.1002/2014GL061378, 2014.
Cooper, O. R., Gao, R.-S., Tarasick, D., Leblanc, T., and Sweeney, C.: Long-term ozone trends at rural ozone monitoring sites across the United States, 1990–2010, J. Geophys. Res., 117, D22307, https://doi.org/10.1029/2012JD018261, 2012.
Cooper, O. R., Parrish, D. D., Ziemke, J., Balashov, N. V., Cupeiro, M., Galbally, I. E., Gilge, S., Horowitz, L., Jensen, N. R., Lamarque, J.-F., Naik, V., Oltmans, S. J., Schwab, J., Shindell, D. T., Thompson, A. M., Thouret, V., Wang, Y., and Zbinden, R. M.: Global distribution and trends of tropospheric ozone: An observation-based review, Elementa Sci. Anthropocene, 2, 000029, https://doi.org/10.12952/journal.elementa.000029, 2014.
Crippa, M., Solazzo, E., Huang, G., Guizzardi, D., Koffi, E., Muntean, M., Schieberle, C., Friedrich, R., and Janssens-Maenhout, G.: High resolution temporal profiles in the Emissions Database for Global Atmospheric Research, Sci. Data, 7, 121, https://doi.org/10.1038/s41597-020-0462-2, 2020.
Eyring, V., Bony, S., Meehl, G. A., Senior, C. A., Stevens, B., Stouffer, R. J., and Taylor, K. E.: Overview of the Coupled Model Intercomparison Project Phase 6 (CMIP6) experimental design and organization, Geosci. Model Dev., 9, 1937–1958, https://doi.org/10.5194/gmd-9-1937-2016, 2016.
Fowler, D., Amann, M., Anderson, R., Ashmore, M., Cox, P., Depledge, M., Derwent, D., Grennfelt, P., Hewitt, N., Oystein, H., Jenkin, M., Kelly, F., Liss, P., Pilling, M., Pyle, J., Slingo, J., and Stevenson, D.: Ground-level ozone in the 21st century: future trends, impacts and policy implications, The Royal Society, London, 11, ISBN 978-0-85403-713-1, 2008.
Griffiths, P. T., Murray, L. T., Zeng, G., Shin, Y. M., Abraham, N. L., Archibald, A. T., Deushi, M., Emmons, L. K., Galbally, I. E., Hassler, B., Horowitz, L. W., Keeble, J., Liu, J., Moeini, O., Naik, V., O'Connor, F. M., Oshima, N., Tarasick, D., Tilmes, S., Turnock, S. T., Wild, O., Young, P. J., and Zanis, P.: Tropospheric ozone in CMIP6 simulations, Atmos. Chem. Phys., 21, 4187–4218, https://doi.org/10.5194/acp-21-4187-2021, 2021.
Guenther, A., Hewitt, C. N., Erickson, D., Fall, R., Geron, C., Graedel, T., Harley, P., Klinger, L., Lerdau, M., Mckay, W. A., Pierce, T., Scholes, B., Steinbrecher, R., Tallamraju, R., Taylor, J., and Zimmerman, P.: A global model of natural volatile organic compound emissions, J. Geophys. Res.-Atmos., 100, 8873–8892, https://doi.org/10.1029/94JD02950, 1995.
Hoesly, R. M., Smith, S. J., Feng, L., Klimont, Z., Janssens-Maenhout, G., Pitkanen, T., Seibert, J. J., Vu, L., Andres, R. J., Bolt, R. M., Bond, T. C., Dawidowski, L., Kholod, N., Kurokawa, J.-I., Li, M., Liu, L., Lu, Z., Moura, M. C. P., O'Rourke, P. R., and Zhang, Q.: Historical (1750–2014) anthropogenic emissions of reactive gases and aerosols from the Community Emissions Data System (CEDS), Geosci. Model Dev., 11, 369–408, https://doi.org/10.5194/gmd-11-369-2018, 2018.
Hogrefe, C., Hao, W., Zalewsky, E. E., Ku, J.-Y., Lynn, B., Rosenzweig, C., Schultz, M. G., Rast, S., Newchurch, M. J., Wang, L., Kinney, P. L., and Sistla, G.: An analysis of long-term regional-scale ozone simulations over the Northeastern United States: variability and trends, Atmos. Chem. Phys., 11, 567–582, https://doi.org/10.5194/acp-11-567-2011, 2011.
HTAP: Hemispheric Transport of Air Pollution 2010, Part A: Ozone and Particulate Matter, Air Pollution Studies No. 17, edited by: Dentener, F., Keating, T., and Akimoto, H., United Nations, New York and Geneva, 978-92-1054-1-091, 2010.
Jaidan, N., El Amraoui, L., Attié, J.-L., Ricaud, P., and Dulac, F.: Future changes in surface ozone over the Mediterranean Basin in the framework of the Chemistry-Aerosol Mediterranean Experiment (ChArMEx), Atmos. Chem. Phys., 18, 9351–9373, https://doi.org/10.5194/acp-18-9351-2018, 2018.
Li, K., Jacob, D. J., Shen, L., Lu, X., De Smedt, I., and Liao, H.: Increases in surface ozone pollution in China from 2013 to 2019: anthropogenic and meteorological influences, Atmos. Chem. Phys., 20, 11423–11433, https://doi.org/10.5194/acp-20-11423-2020, 2020.
Lin, M., Horowitz, L. W., Cooper, O. R., Tarasick, D., Conley, S., Iraci, L. T., Johnson, B., Leblanc, T., Petropavlovskikh, I., and Yates, E. L.: Revisiting the evidence of increasing springtime ozone mixing ratios in the free troposphere over western North America, Geophys. Res. Lett., 42, 8719–8728, https://doi.org/10.1002/2015GL065311, 2015.
Lin, M., Horowitz, L. W., Payton, R., Fiore, A. M., and Tonnesen, G.: US surface ozone trends and extremes from 1980 to 2014: quantifying the roles of rising Asian emissions, domestic controls, wildfires, and climate, Atmos. Chem. Phys., 17, 2943–2970, https://doi.org/10.5194/acp-17-2943-2017, 2017.
Logan, J. A.: Tropospheric ozone: Seasonal behavior, trends and anthropogenic influences, J. Geophys. Res., 90, 10463–10482, 1985.
Marenco, A., Gouget, H., Nédélec, P., Pagés, J.-P., and Karcher, F.: Evidence of a long-term increase in tropospheric ozone from Pic du Midi data series: Consequences: Positive radiative forcing, J. Geophys. Res., 99, 16617–16632, https://doi.org/10.1029/94JD00021, 1994.
Meinshausen, M., Vogel, E., Nauels, A., Lorbacher, K., Meinshausen, N., Etheridge, D. M., Fraser, P. J., Montzka, S. A., Rayner, P. J., Trudinger, C. M., Krummel, P. B., Beyerle, U., Canadell, J. G., Daniel, J. S., Enting, I. G., Law, R. M., Lunder, C. R., O'Doherty, S., Prinn, R. G., Reimann, S., Rubino, M., Velders, G. J. M., Vollmer, M. K., Wang, R. H. J., and Weiss, R.: Historical greenhouse gas concentrations for climate modelling (CMIP6), Geosci. Model Dev., 10, 2057–2116, https://doi.org/10.5194/gmd-10-2057-2017, 2017.
Parrish, D. D., Law, K. S., Staehelin, J., Derwent, R., Cooper, O. R., Tanimoto, H., Volz-Thomas, A., Gilge, S., Scheel, H.-E., Steinbacher, M., and Chan, E.: Long-term changes in lower tropospheric baseline ozone concentrations at northern mid-latitudes, Atmos. Chem. Phys., 12, 11485–11504, https://doi.org/10.5194/acp-12-11485-2012, 2012.
Parrish, D. D., Law, K. S., Staehelin, J., Derwent, R., Cooper, O. R., Tanimoto, H., Volz-Thomas, A., Gilge, S., Scheel, H.-E., Steinbacher, M., and Chan, E.: Lower tropospheric ozone at northern midlatitudes: Changing seasonal cycle, Geophys. Res. Lett., 40, 1631–1636, https://doi.org/10.1002/grl.50303, 2013.
Parrish, D. D., Lamarque, J. F., Naik, V., Horowitz, L., Shindell, D. T., Staehelin, J., Derwent, R., Cooper, O. R., Tanimoto, H., Volz-Thomas, A., Gilge, S., Scheel, H.-E., Steinbacher, M., and Fröhlich, M.: Long-term changes in lower tropospheric baseline ozone concentrations: Comparing chemistry-climate models and observations at northern midlatitudes, J. Geophys. Res.-Atmos., 119, 5719–5736, https://doi.org/10.1002/2013JD021435, 2014.
Parrish, D. D., Galbally, I. E., Lamarque, J.-F., Naik, V., Horowitz, L., Shindell, D. T., Oltmans, S. J., Derwent, R., Tanimoto, H., Labuschagne, C., and Cupeiro, M.: Seasonal cycle of O3 in the marine boundary layer: Observation and model simulation comparisons, J. Geophys. Res.-Atmos., 121, 538–557, https://doi.org/10.1002/2015JD024101, 2016.
Parrish, D. D., Young, L. M., Newman, M. H., Aikin, K. C., and Ryerson, T. B.: Ozone design values in Southern California's air basins: Temporal evolution and U. S. back-ground contribution, J. Geophys. Res.-Atmos., 122, 11166–11182, https://doi.org/10.1002/2016JD026329, 2017.
Parrish, D. D., Derwent, R. G., O'Doherty, S., and Simmonds, P. G.: Flexible approach for quantifying average long-term changes and seasonal cycles of tropospheric trace species, Atmos. Meas. Tech., 12, 3383–3394, https://doi.org/10.5194/amt-12-3383-2019, 2019.
Parrish, D. D., Derwent, R. G., Steinbrecht, W., Stübi, R., VanMalderen, R., Steinbacher, M., Trickl, T., Ries, L., and Xu, X.: Zonal similarity of long-term changes and seasonal cycles of baseline ozone at northern midlatitudes, J. Geophys. Res.-Atmos., 125, e2019JD031908, https://doi.org/10.1029/2019JD031908, 2020.
Rasmussen, D. J., Hu, J., Mahmud A., and Kleeman, M. J.: The Ozone–Climate Penalty: Past, Present, and Future, Environ. Sci. Technol., 47, 24, 14258–14266, https://doi.org/10.1021/es403446m, 2013.
Rieder, H. E., Fiore, A. M., Clifton, O. E., Correa, G., Horowitz, L. W., and Naik, V.: Combining model projections with site-level observations to estimate changes in distributions and seasonality of ozone in surface air over the U. S. A., Atmos. Environ., 193, 302–315, https://doi.org/10.1016/j.atmosenv.2018.07.042, 2018.
Schnell, J. L., Prather, M. J., Josse, B., Naik, V., Horowitz, L. W., Zeng, G., Shindell, D. T., and Faluvegi, G.: Effect of climate change on surface ozone over North America, Europe, and East Asia, Geophys. Res. Lett., 43, 3509–3518, https://doi.org/10.1002/2016GL068060, 2016.
Schultz, M. G., Schröder, S., Lyapina, O., et al.: Tropospheric ozone assessment report: Database and metrics data of global surface ozone observations, Elementa, 5, 58, https://doi.org/10.1525/elementa.244, 2017 (data available at: https://toar-data.org, last access: 20 August 2020).
Simon, H., Reff, A., Wells, B., Xing, J., and Frank, N.: Ozone Trends Across the United States over a Period of Decreasing NOx and VOC Emissions, Environ. Sci. Technol., 49, 186–195, https://doi.org/10.1021/es504514z, 2014.
Strode, S. A., Rodriguez, J. M., Logan, J. A., Cooper, O. R., Witte, J. C., Lamsal, L. N., Damon, M., Van Aartsen, B., Steenrod, S. D., and Strahan, S. E.: Trends and variability in surface ozone over the United States, J. Geophys. Res.-Atmos., 120, 9020–9042, https://doi.org/10.1002/2014JD022784, 2015.
van Marle, M. J. E., Kloster, S., Magi, B. I., Marlon, J. R., Daniau, A.-L., Field, R. D., Arneth, A., Forrest, M., Hantson, S., Kehrwald, N. M., Knorr, W., Lasslop, G., Li, F., Mangeon, S., Yue, C., Kaiser, J. W., and van der Werf, G. R.: Historic global biomass burning emissions for CMIP6 (BB4CMIP) based on merging satellite observations with proxies and fire models (1750–2015), Geosci. Model Dev., 10, 3329–3357, https://doi.org/10.5194/gmd-10-3329-2017, 2017.
Wild, O., Voulgarakis, A., O'Connor, F., Lamarque, J.-F., Ryan, E. M., and Lee, L.: Global sensitivity analysis of chemistry–climate model budgets of tropospheric ozone and OH: exploring model diversity, Atmos. Chem. Phys., 20, 4047–4058, https://doi.org/10.5194/acp-20-4047-2020, 2020.
Young, P. J., Archibald, A. T., Bowman, K. W., Lamarque, J.-F., Naik, V., Stevenson, D. S., Tilmes, S., Voulgarakis, A., Wild, O., Bergmann, D., Cameron-Smith, P., Cionni, I., Collins, W. J., Dalsøren, S. B., Doherty, R. M., Eyring, V., Faluvegi, G., Horowitz, L. W., Josse, B., Lee, Y. H., MacKenzie, I. A., Nagashima, T., Plummer, D. A., Righi, M., Rumbold, S. T., Skeie, R. B., Shindell, D. T., Strode, S. A., Sudo, K., Szopa, S., and Zeng, G.: Pre-industrial to end 21st century projections of tropospheric ozone from the Atmospheric Chemistry and Climate Model Intercomparison Project (ACCMIP), Atmos. Chem. Phys., 13, 2063–2090, https://doi.org/10.5194/acp-13-2063-2013, 2013.