In-situ observations are essential to improve our knowledge on the chemical composition of the atmosphere and its evolution with time, and to validate models and satellite observations. While the network of surface stations has considerably expanded over the last decades (although not in all regions of the world), in-situ observations still remain much sparser in altitude. Besides dedicated aircraft research campaigns that provide a detailed view of the chemical composition of the atmosphere but with a limited spatio-temporal coverage, routine in-situ measurements still essentially rely on radiosondes and commercial aircraft. Ozone (O3) soundings began in the early 1960s and now provide a few thousand vertical profiles per year at several dozens stations throughout the world.
Routine in-situ airborne observations of chemical species not restricted to O3 – e.g. carbon monoxide (CO), nitrogen oxides (NOx), carbon dioxide (CO2), methane (CH4) – rely on only a few programs conducting airborne measurements using in-service aircraft since the 1990s. Among the programs still on-going, the oldest is the CONTRAIL (Comprehensive Observation Network for TRace gases by AIrLiner) program, within which greenhouse gases (CO2, CH4, N2O, SF6) measurements have been performed since 1993 using Boeing aircraft operated by Japan Airlines (Machida et al., 2008). Initiated in 1994, the MOZAIC (Measurement of OZone and water vapour by AIrbus in-service airCraft) program consisted in measuring O3, CO and water vapour worldwide and routinely using as platform five in-service Airbus (A330/A340) long-haul aircraft operated by several international airlines (Marenco et al., 1998). In the framework of the CARIBIC (Civil Aircraft for the Regular Investigation of the atmosphere Based on an Instrument Container) program, a much larger number of chemical species and physical parameters were measured from an instrumented cargo container installed on an Airbus aircraft from Lufthansa, for 4 flights per month (Brenninkmeijer et al., 2007). In 2005, MOZAIC and CARIBIC were joined in the preparatory phase of the European Research Infrastructure called IAGOS (In Service Aircraft for Global Observing System; Petzold et al., 2015) operational since 2011, which includes two branches: IAGOS-CORE (ex-MOZAIC) and IAGOS-CARIBIC. New instrumental developments were conducted in IAGOS-CORE and now allow the measurement of nitrogen oxides (NOx) (on one aircraft from Lufthansa) (Berkes et al., in preparation) and in the near future (aeronautical certification of the instrument already approved) greenhouse gases (CO2, CH4) (Filges et al., 2015), while developments for aerosol measurements are still on-going (Bundke et al., 2015).
So far, many studies have used the IAGOS data to investigate air pollution throughout the troposphere, including the planetary boundary layer (PBL) (e.g. Ding et al., 2008; Elguindi et al., 2010; Kalabokas et al., 2007, 2013; Petetin et al., 2016a, 2016b; Sahu et al., 2014; Sauvage et al., 2005; Sheel et al., 2016; Tressol et al., 2008; Yamasoe et al., 2015). However, a part of the scientific community seems reluctant to use the IAGOS data for studying the lowermost PBL due to concerns about the representativeness of the IAGOS measurements close to the surface. While ozonesondes are usually launched in remote, rural or low-density urban areas, the specificity of the IAGOS measurements relies on the fact that the ascent/descent profiles are (i) slanted rather than strictly vertical, (ii) performed close to international airports (with potentially high emissions on the tarmac) (iii) located in the vicinity of large cities (among the 290 airports visited since 1994, the average population of the nearby city is 1.6 millions inhabitants), and (iv) along flight corridors frequented by other aircraft. For these reasons, questions arise on the representativeness of the IAGOS measurements in the lower troposphere (roughly, the 2 first kilometres). For instance, the Air Quality (AQ) community working on the validation of regional chemistry-transport models (thus focussing on the surface and the PBL) has sometimes argued that the IAGOS data are likely strongly influenced by very local pollution sources (e.g. airport, other aircraft) that cannot be correctly represented in the models with the current spatial resolution (a few kilometres). This would prevent relevant model-observation comparisons, in the same way that urban traffic surface stations are rejected for the validation of models at the surface (contrary to rural and urban background stations). However, the situation changed over the last years with model inter-comparison programs like AQMEII (Air Quality Model Evaluation International Initiative) or CAMS (Copernicus Atmospheric Monitoring Service) that benefited from the IAGOS dataset to evaluate models in the lower troposphere (e.g. Elguindi et al., 2010; Solazzo et al., 2013). Another example is given by the community working on the validation of CO tropospheric columns observed by satellite. Although several studies have used the IAGOS profiles to evaluate satellite products, mostly for CO (e.g. Clerbaux et al., 2008; Emmons et al., 2009; Worden et al., 2010), there are still concerns about the influence of these local pollution sources on the IAGOS observations close to the surface (where CO is the most concentrated) and thus on the pertinence of their use for the evaluation of satellite products (considering the fact that pixels have a typical size of a few tens of kilometres). Considering the scarcity of in-situ observations in altitude in the troposphere, there is therefore a strong need for a comprehensive study of the potential influence of the different local emissions (e.g. airport, other aircraft, nearby agglomeration) to assess the representativeness of IAGOS observations in the lower troposphere. This is required to better identify the type of applications allowed by the IAGOS dataset. Such analysis is of primary importance since, compared to the ~68,000 ozone soundings (since 1924) publicly available in the World Ozone and Ultraviolet Radiation Data Centre (WOUDC) database, the IAGOS database now represents about 70,000 O3 profiles since 1994 and 40,000 CO profiles since 2002 which, thus, contributes a large proportion of the whole dataset of in-situ profiles available in the troposphere.
Over the last two decades, several studies have investigated the consistency of the IAGOS O3 dataset with radiosondes and surface stations (Thouret et al., 1998; Chevalier et al., 2007; Logan et al., 2012; Tilmes et al., 2012; Zbinden et al., 2013; Staufer et al., 2013, 2014; Tanimoto et al., 2015). The most recent and comprehensive study was made by Tanimoto et al. (2015), who compared collocated O3 measurements (in space and time) obtained from IAGOS aircraft, ozonesondes and GAW (Global Atmospheric Watch) surface stations. Good correlations were obtained between surface stations and ozonesondes in the first 200 m (r = 0.8–1.0). Correlations were lower between surface stations and IAGOS (r ~ 0.6–0.8), likely due to the larger distance between sites compared with sondes (40–80 km), in agreement with Liu et al. (2009). These correlations were substantially improved after applying a simple wind selection (wind direction at ±15° of the direction between the two locations, and wind speed above 2 m s–1). In the first kilometre, a good consistency was found between the radiosondes and the IAGOS data profiles, with median relative differences around ±2%. Although this study greatly improved our confidence in the representativeness of the IAGOS O3 measurements, a similar assessment of the representativeness of the IAGOS CO measurements is still missing. In addition, for the comparison between IAGOS and other datasets, some airports like Frankfurt (not taken into account in Tanimoto et al. (2015)) offer a much larger number of profiles, which can allow more in-depth analysis.
Although its secondary sources (oxidation of CH4 and non-methanic volatile organic compounds (NMVOCs)) account for a large part of its global budget (around 57% of the total source (Stein et al., 2014)), CO is characterized by strong emissions associated with all types of incomplete combustion and a long lifetime (from a few weeks to a few months), which traditionally makes it a very useful tracer of pollution (Heald et al., 2003; Liu et al., 2003). Conversely, O3 is a secondary pollutant, formed by a complex chemical mechanism involving notably NOx, VOCs and CO, and likely to be quickly removed by surface dry deposition (Monks et al., 2015).
The overall objective of this study is to investigate more deeply the representativeness of the IAGOS O3 and CO measurements in the lower troposphere. More specifically, this study aims at analysing how such airborne measurements are comparable to the surface observations measured by the nearby AQ monitoring network (AQN). Despite (usually) larger distances from the IAGOS airports, the comparisons will be extended to the GAW stations in order to assess how much the IAGOS observations throughout the PBL are influenced by the regional background. The subsequent objective of this study is to give recommendations on the possible use of the IAGOS dataset in the lower troposphere. The open research questions are: (i) are they relevant for the study of the AQ at the scale of the agglomeration? (ii) are they better suited for quantifying the impact of airborne activities on the local AQ? or (iii) are they able to provide information on the background pollution affecting the agglomeration?
The study will focus on Frankfurt, Germany, airport where IAGOS observations are the most abundant, but some insights from two other European airports at Vienna, Austria, and Paris, France, will be given. Both O3 and CO are included. The analysis is done over 11 years between 2002 and 2012. The data and methods used in this study are described in Sect. 2. Results are analysed in Sect. 3, and summarized and discussed in Sect. 4.
This study mostly relies on the O3 and CO observations available in the framework of the MOZAIC-IAGOS program (http://www.iagos.org) (Marenco et al., 1998; Petzold et al., 2015). Observations have been performed by commercial aircraft from several airlines since 1994 for O3 and 2002 for CO. In both the MOZAIC and IAGOS programs, the same instruments are used in all aircraft. During the 2011–2014 overlapping years, inter-comparisons were systematically performed between the MOZAIC equipped aircraft and the IAGOS fleet, demonstrating a good consistency in the dataset (Nédélec et al., 2015). In MOZAIC, O3 was measured using a dual-beam UV-absorption monitor (time resolution of 4 seconds) with an accuracy/precision estimated at about ±2 ppbv/±2% (Thouret et al., 1998), while CO was measured by an improved infrared filter correlation instrument (time resolution of 30 seconds) with an accuracy/precision estimated at ±5 ppbv/±5% (Nédélec et al., 2003). In IAGOS, both compounds are measured with instruments based on the same technology used for MOZAIC, with the same estimated accuracy and the same data quality control. A more detailed description of the IAGOS system and its validation can be found in Nédélec et al. (2015).
We use the barometric altitude available in the IAGOS database. It is deduced from the pressure measured by the aircraft, assuming standard conditions at the surface (temperature of 288.15 K, pressure of 1013.25 hPa). It is worth noting that this leads to an uncertainty on the actual altitude of the aircraft above the surface. In particular, under specific atmospheric conditions (cyclone), this barometric altitude can thus sometimes be located below the actual airport altitude. To tackle this uncertainty, it would be useful in the future to take into account the real conditions of temperature and pressure observed at the surface based on meteorological stations available in or around the airport. For now, such developments are yet not available and in this study, we will therefore consider all IAGOS measurements associated to their altitude above sea level (ASL), no matter if the altitude is below the actual elevation of the airport. Note also that the GPS altitude (measured by the aircraft system) is now available in the IAGOS dataset, but only since late 2014.
It is also worth noting that IAGOS profiles are not exactly vertical. The ascent/descent rates of IAGOS aircraft are 7.3 ± 2.0 m s–1 on average, i.e. 9 min to reach an altitude of 4 km. In parallel, the aircraft’s horizontal speed (available in the IAGOS database) increases with altitude from about 85 m s–1 at 0–1 km to 166 m s–1 at 3–4 km on average. The horizontal distance between Frankfurt airport and IAGOS aircraft depending on the aircraft altitude is plotted in Figure 1. On average over the period 2002–2012, this leads to an horizontal displacement of IAGOS aircraft of about 9 ± 3, 19 ± 4, 36 ± 10, 41 ± 16, 71 ± 15 and 92 ± 17 km to reach an altitude of 0.5, 1, 2, 3, 4 and 5 km, respectively. Therefore, the IAGOS profiles have to be considered as semi-vertical profiles. However, it is worth noting that they can be considered as vertical profiles in model or satellite validation if the horizontal resolution (or the size of the pixel) is coarse enough (roughly, 1° for the 4 km above surface, 0.5° for the 2 km above surface, at mid-latitudes). For finer resolutions, the semi-verticality of IAGOS profiles has to be taken into account.
Surface O3 and CO data from the local AQN are taken from the AIRBASE database (https://www.eea.europa.eu/data-and-maps/data/airbase-the-european-air-quality-database-7). AIRBASE data are available until January 2012. For comparison, some results in two other European cities, Vienna and Paris, will also be discussed. These two cities are chosen because they offer the largest number of IAGOS profiles (after Frankfurt) and a dense network of surface stations. For Paris, instead of AIRBASE, data are taken directly from AIRPARIF, the local agency in charge of the air quality monitoring network (https://www.airparif.asso.fr, data downloaded the 20th July 2017). In addition, we also use the CO and O3 measurements available at GAW stations in West-Central Europe (see Table 1) in order to investigate the representativeness of IAGOS at a regional scale. GAW data are taken from the World Data Centre for Greenhouse Gases (WDCGG) (Schultz et al., 2015) (http://ds.data.jma.go.jp/gmd/wdcgg/; data downloaded the 1st of July 2016). Most of the GAW stations are located at less than 500 km from Frankfurt (the only exception being the Krvavec station 620 km away). At all these surface stations, O3 is measured by UV absorption. The CO measurements usually rely on the techniques based on infrared absorption.
|Station name (contributor*)||Short name||Location||Elevation|
|Jungfraujoch (Empa)||JFJ||7.987°E, 46.548°N||3580 m|
|Sonnblick (EAA)||SNB||12.95°E, 47.05°N||3106 m|
|Krvavec (ARSO)||KVV||14.53°E, 46.30°N||1720 m|
|Schauinsland (UBA)||SSL||7.92°E, 47.92°N||1205 m|
|Rigi (Empa)||RIG||8.45°E, 47.06°N||1031 m|
|Hohenpeissenberg (DWD)||HPB||11.02°E, 47.8°N||985 m|
|Kosetice (CHMI)||KOS||15.08°E, 49.58°N||534 m|
|Payerne (Empa)||PAY||6.95°E, 46.82°N||490 m|
|Neuglobsow (UBA)||NGL||13.03°E, 53.17°N||65 m|
|Kollumerwaard (RIVM)||KMW||6.28°E, 53.33°N||0 m|
AQN include three main types of stations: (i) urban traffic stations located close to traffic emissions, usually at the kerbside, (ii) urban background stations located within the city or its suburbs (sometimes referred as suburban background stations) but further from the direct influence of traffic emissions (i.e. usually in a square or a small garden) with a typical representativeness ranging from a few km2 to some tens km2, and (iii) rural background stations located outside the city, and considered to have a representativeness of some hundreds of km2. In this study, we will not distinguish urban background and suburban background stations, as differences among them are usually small compared with the two other types of stations. For clarity, a label is added to the name of each AQN station: “_R” for rural background, “_U” for urban background and “_T” for traffic.
Figure 2 shows the location of the GAW stations as well as the location of all surface stations around each airport. At Frankfurt (and nearby cities), the local AQN includes 16 surface stations: 1 rural background station, 9 urban background stations and 6 traffic stations. Note that due to several errors about the information relative to stations in AIRBASE, the type of station (e.g. traffic, urban/rural background) is identified directly from the German Federal Environmental Agency (Umwelt Bundesamt, http://www.env-it.de/stationen/public/stationList.do). Only 3 stations are located within the Frankfurt agglomeration, the other being located in nearby agglomerations: Mainz, Wiesbaden, Rüsselsheim and Darmstadt. At Vienna, 18 stations are considered, including 2 rural background stations, 12 urban background stations and 4 traffic stations. At Paris, 35 stations are taken into account, including 8 rural background stations, 21 urban background stations and 6 traffic stations. Information on the location and the altitude of all these surface stations are given in Table S-1 in the Supplement. Note that the same colours used in Figure 2 to represent the different types of surface stations (green for GAW stations; purple, blue and red for rural background, urban background and traffic stations from the AQN, respectively) will be used in all the following figures.
Over the 2002–2012 period, a total of 12,569 ascent/descent profiles are available at Frankfurt airport (2,054 at Vienna and 1,610 at Paris). For information purposes, the location of IAGOS observations around airports is shown in the Supplement (Figures S-1 to S-3). In order to facilitate the comparisons with surface stations, IAGOS data are aggregated at the hourly scale over 50 m-deep layers from 0 to 4 km ASL from the raw IAGOS data (for instance, the “175 m” label will thus refer to the altitude layer ranging from 150 to 200 m ASL). At all surface stations, O3 and CO mixing ratios are downloaded in the format of hourly averages. Surface stations give real hourly averages corresponding to the average of all quasi-instantaneous measurements of the instrument during a specific hour. However, it is worth noting that the hourly aggregates of IAGOS data do not correspond to hourly averages as one specific hourly value may be based on only one flight crossing the 50 m-deep layer in a few seconds, i.e. on only a few quasi-instantaneous observations. For convenience, for both airborne and surface data, we will refer indistinctly to hourly data in the paper but the reader should keep in mind that the IAGOS hourly averages are somewhat artificial.
The IAGOS measurements are sporadic in time, as they depend on the number of aircraft flying. Over the period 2002–2012, the mean number of ascent/descent profiles with available CO and/or O3 data per day is 2 at Frankfurt airport (the maximum is 8 flights per day). Excluding the periods of technical failure in the system by considering only the days with at least one flight, this number increases to 3 flights per day on average. In terms of time of departure/arrival, the IAGOS flights at Frankfurt are mostly between 03:00 and 18:00 UTC, with almost no flight between 00:00 and 03:00 UTC. More details can be found in Petetin et al. (2016b). The comparison between IAGOS and surface data is made considering only the hours with simultaneous airborne and surface data (i.e. no time shift between them is allowed). Unless otherwise specified, all average CO and O3 mixing ratios at surface stations discussed in this paper are calculated taking into account only the data when IAGOS flights took place. At a given hour, the availability of IAGOS data is not necessary the same at all levels (since for instance, an ascent profile may start at 14:59 at the surface and reach 4 km ASL at 15:08). Thus, surface data are considered when at least one IAGOS observation is available between 0 and 4 km ASL. Some comparisons between the two datasets are also made at the daily and monthly scale. For these analysis, hourly data are aggregated and averaged daily and monthly, without any minimum data coverage required. These daily and monthly data are used only for comparison, but do not correspond to real daily and monthly averages as they only include data sampled simultaneously by both aircraft and surface stations. Monthly time series of both CO and O3 from each dataset are plotted in Figures S-4 to S-5 in the Supplement. Over the period 2002–2012 (4,018 days or 96,432 hours at total), the comparison is thus performed on 9% of the hourly dataset (8,348 hours). At daily and monthly scales, the availability of IAGOS data increases to 75 and 88%, respectively. A roughly similar amount of IAGOS data is available during all four seasons (for O3: 24% in winter, 20% in spring and summer, 23% in autumn).
The distribution of CO and O3 hourly mixing ratios over the period 2002–2012 is shown in Figure 3 for all surface stations and a subset of IAGOS altitude levels below 4 km ASL. In terms of CO pollution, a clear distinction among the 3 different types of surface stations is highlighted. On average, the CO mixing ratio is 630 ± 414 ppbv (mean standard deviation of the different stations) at traffic stations, 348 ± 212 ppbv at urban background stations, and 171 ± 61 ppbv at GAW stations. As previously mentioned (see Sect. 2.3), these averages are calculated based on the hourly surface data with concomitant IAGOS flights. Such differences between the different types of stations are expected considering the increasing distance to strong emission sources like traffic. At the 3 first altitude levels (0–50, 50–100, 100–150 m ASL), the IAGOS measurements give a CO mixing ratio of 292 ± 142, 261 ± 124 and 244 ± 109 ppbv, respectively. This is the first important result: at Frankfurt, even at the lowest altitude levels, the CO mixing ratios measured by IAGOS aircraft never reach mixing ratios as high as measured at traffic stations, but roughly correspond to the urban background pollution measured in the nearby cities and are even slightly lower by 16, 25 and 30% in these 3 first levels, respectively. We calculated the relative bias of IAGOS versus surface stations from the local AQN considering simultaneously all individual hourly data from surface stations with concomitant IAGOS data at the corresponding altitudes (i.e. the station elevation). The overall bias on CO reaches –26% for urban background stations, and –61% for traffic stations (more details on this bias are given below in Sect. 3.2).
As mentioned in Sect. 2.3, contrary to surface stations, the IAGOS data used here are based on hourly aggregates of sporadic (quasi-)instantaneous observations. Compared with surface data, its temporal variability (represented by the standard deviation) may thus be biased high since it includes not only the sub-hourly variability but also a part of the instrument noise (smoothed in the surface hourly averages). Despite that, IAGOS shows close to the surface a temporal variability much lower than the variability observed at the surface stations (by a factor of 1.5–2 in the 3 first altitude levels). The second important result is that the CO mixing ratios quickly decrease with altitude, and reach the average mixing ratio of GAW stations (171 ± 61 ppbv) at 650–700 m ASL. A similar picture is obtained at the seasonal scale (not shown). Interestingly, the altitude levels at which IAGOS reaches the average CO given by the GAW stations slightly varies with the season, from about 650 m in winter/autumn to 750 m in spring/summer. This is consistent with the seasonal variations of the PBL height. More details on the comparison between IAGOS and GAW are given below in Sect. 3.3.
The distribution of hourly O3 mixing ratios is shown in Figure 3 (bottom panel). Note that due to the fast titration of O3 by the NO emitted by car engines, traffic stations usually do not measure O3. The mean O3 mixing ratio is 19 ± 17 ppbv at the urban background stations and 35 ± 15 ppbv at the (unique) rural background station of the AQN. For the GAW stations, mixing ratios range between 26 ± 13 ppbv at lowest elevations (KMW, 0 m) and 52 ± 10 ppbv at the highest (JFJ, 3580 m). The mean O3 mixing ratios observed by IAGOS in the first 3 altitude levels are 17 ± 16, 20 ± 17 and 20 ± 16 ppbv, respectively. The corresponding relative differences with the mean urban background O3 mixing ratios are thus –7, +8 and +10%. Comparing all individual hourly data with concomitant IAGOS data at the corresponding altitudes, the mean difference between IAGOS and surface O3 is +3% for urban background stations. Thus, as for CO, the O3 measured by IAGOS aircraft close to the surface appears close to the urban background measured by surface stations. The mean O3 measured at the rural background station DEHE052_R is much higher (35 ± 15 ppbv), but this is due to its location in the Taunus observatory at the summit of Kleiner Feldberg (elevation of 811 m), as discussed in Sect. 3.3. At this altitude, IAGOS shows O3 mixing ratios only 12% higher than DEHE052_R, thus in reasonable agreement.
As mentioned in Sect. 3.1, the exact comparison between IAGOS and urban background stations gives small differences. Reasonable correlations are also found between the two datasets (r = 0.58 and 0.81 for CO and O3, respectively). In this section, we investigate the diurnal variability of these differences. The biases between the two datasets are calculated for each hour of the day, and are plotted in Figure 4. Here, the bias designates IAGOS minus the urban background stations. These biases show a substantial diurnal variability. Both the negative bias of CO and the positive bias of O3 at urban background stations are greater (in absolute value) during the morning (06:00–09:00 local time (LT = UTC+1)) when they reach –40% for CO and +70% for O3. After 10:00 LT, these biases get smaller until a minimum is reached during afternoon, when they range between ±20% for both CO and O3. They increase again in late afternoon (up to ±40%). For O3, the bias is not significant during the afternoon. The correlation follows similar diurnal variations with a minimum during the early morning (0.4–0.6) and a maximum during the afternoon/evening (0.7–0.9).
In these comparisons, we considered the IAGOS data at the altitudes corresponding to the elevations of the urban background stations, which range between ±50 m around the elevation of the Frankfurt airport (see the zoom panel in Figure 5). Thus, even during nighttime, early morning or late afternoon, most of these IAGOS observations likely still belong to the boundary layer (i.e. we are not comparing observations at the surface with observations in the nocturnal residual layer). Therefore, the diurnal variations of the differences between IAGOS and urban background stations, and more specifically the stronger discrepancies during early morning and late afternoon, are likely more explained by the combined effect of higher local emissions and less dispersive conditions. Indeed, these times of the day correspond to the well-known morning and evening peaks of traffic emissions (rush hours). Although these urban background stations are not located at the kerbside like traffic stations, they are still greatly influenced by traffic emissions that represent one of the major sources of pollution, as illustrated by the diurnal variations of CO or NOx (not shown). These traffic emissions increase the CO mixing ratios (more emissions) and decrease the O3 (through a stronger titration by the NO emitted by the vehicles). In parallel, the PBL is not fully developed and the (horizontal and vertical) mixing within the PBL still moderate, which may hinder the dispersion of the local pollution.
Note that focusing only on the 12:00–17:00 LT time window, the mean difference between IAGOS and urban background stations reaches –14 and –4% for CO and O3, respectively (compared to –26 and +3% when all data are taken into account). Since we are interested in investigating the representativeness of the whole IAGOS dataset, we will keep considering all data whatever the time of the day in the rest of the paper, although some insights during the 12:00–17:00 LT time window will be given for information purpose.
The CO mixing ratio is plotted against altitude for IAGOS measurements and elevation of the surface stations in the lowest troposphere in Figure 5 (top panel). Due to differences of elevation (from 0 m at KMW to 3,580 m at JFJ) and nearby environment (e.g. site in low-density urban area, coastal site, mountain site), the CO pollution varies strongly from one GAW station to the other. Substantial differences between IAGOS and GAW data are observed below 1 km. Compared to IAGOS, the two GAW stations at 500 m (PAY and KOS) show higher CO while the two stations close to 0 m (KMW and NGL) show lower CO mixing ratios. The mixing ratios at all other GAW stations closely follow the IAGOS vertical profile at Frankfurt. A good consistency between IAGOS and GAW is also found during all 4 seasons (not shown). Both IAGOS and GAW data tend to show a decrease of CO with altitude close to the ground. A decrease of CO with altitude is also observed among urban background stations. This feature is not observed at the traffic stations, due to the predominant contribution of the traffic emissions. As discussed in Sect. 3.1, the CO mixing ratios measured by IAGOS are slightly lower than the urban background, but much lower than the CO mixing ratios at traffic stations. Concerning the variations of O3 with altitude (Figure 5, bottom panel), a very good agreement is found between IAGOS and the different surface stations, whatever their elevation, although some discrepancies persist for the lowest GAW stations. These results are consistent with the study of Chevalier et al. (2007) that highlighted over the period 2001–2004 a good coherence between IAGOS O3 vertical profiles and a larger set of surface stations in Europe, but with larger differences at lower altitudes.
The mean seasonal variations of CO and O3 at the different surface stations and IAGOS altitude levels are shown in Figure 6. In terms of mixing ratios, the distinction between the different types of surface stations is again obvious and persists all year round. All surface stations and IAGOS altitude levels show similar seasonal variations with maximum CO in winter, and minimum CO in summer. However, results highlight differences of amplitude in the seasonal cycle. Traffic and urban background stations show a mean relative amplitude (here defined as the maximum minus minimum of the seasonal cycle normalized by the annual average) of 52 ± 15 and 68 ± 4%, respectively. At these stations, the amplitude tends to decrease as the mean CO mixing ratio is increasing. At GAW stations, the relative amplitudes range between 36 to 79%, the lower amplitudes being usually found at higher elevations. A notable exception is the KMW station (0 m ASL) that shows a relative amplitude of only 42%, i.e. comparable to the relative amplitude observed at the highest mountain stations. Concerning IAGOS, the amplitude is the highest (50–55%) in the first 500 m, and quickly decreases with altitude down to 30–35% above 1 km ASL. The bias between IAGOS and urban background stations is found to vary with the season, from about –30% in winter/autumn to –14% in summer (against –26% at the annual scale, see Sect. 3.1). Compared with GAW stations, IAGOS (at the corresponding altitude) usually shows a slightly lower CO relative amplitude (the relative bias of amplitude is –20% on average over all GAW stations), mainly due to slightly lower CO during wintertime (–8%).
For O3, a common seasonal pattern is observed at the surface stations and at altitude, with a broad spring-summer maximum and a minimum in late autumn-early winter. This is in good agreement with other observations in the lower troposphere (Parrish et al., 2013). As for CO, the relative amplitude of the IAGOS dataset quickly decreases with altitude from about 100% close to the surface to 30–40% above 1 km ASL. The relative amplitudes observed at the GAW stations are in close agreement with IAGOS at the corresponding altitude levels (relative mean bias of amplitude of –1%). However, the O3 relative amplitude observed at the urban background stations range between 121–144% (134% on average) and is thus slightly stronger compared to what is observed both by aircraft and GAW stations at these altitudes. This is mainly due to a lower minimum of O3 in winter at the urban background stations. The absolute amplitude (maximum minus minimum) is quite similar to the other datasets. As for CO, the bias on O3 between IAGOS and urban background stations thus depicts some seasonal variations, from +28% in winter to –12% in summer (against +3% at the annual scale, see Sect. 3.1). These higher differences for both CO and O3 in winter could be due to less dispersive conditions during the cold season.
We now investigate how the CO and O3 temporal variability observed in IAGOS airborne measurements is comparable to the variability at the surface. The Pearson correlation coefficients (r) between the surface stations and the different IAGOS altitude levels are shown in Figure 7. These correlations are calculated based on hourly, daily and monthly aggregates.
For CO, the correlations between hourly time series of IAGOS and AQN stations are highest close to the surface (r ~ 0.5–0.7 for urban background stations, r ~ 0.4–0.6 for traffic stations) and decrease with altitude (almost no correlation above 2 km ASL). A different picture is found with the GAW stations. For most GAW stations, the correlation with IAGOS hourly time series is low close to the surface and increases with altitude up to a maximum. Interestingly, the altitude at which this maximum correlation is reached is relatively close to the elevation of the corresponding surface station. To highlight this feature, open circles with crosses are added in Figure 7 at the elevation of the corresponding stations (only for both GAW stations and the rural background station). For instance, the correlation between IAGOS and SSL (HPB) – elevation of 1,205 m (985 m) – is 0.16 (0.22) at the lowest altitude level and increases up to 0.64 (0.60) at 1,325 m (875 m) ASL. The main exception is the KOS station that is poorly correlated with IAGOS data whatever the altitude. This result indicates that at a given altitude, the CO variability is reasonably homogeneous at the regional scale in this part of Europe. It is worth noting that these low to moderate correlations are expected at the hourly scale, as we are comparing data sampled at quite distant locations. When considering daily and monthly time series, the correlations are all strongly enhanced but the shape of the profiles remains the same. Note that the high correlations observed at the monthly scale are driven by the seasonal variations. Considering deseasonalized monthly time series, we obtained correlations roughly comprised in the range between the previous daily and monthly correlations (not shown). Thus, this is another important result: the IAGOS observations in the lowest troposphere around Frankfurt share a large part of their variability with the nearby surface stations, likely due to common processes driving CO mixing ratios (e.g. local emissions and meteorology including PBL dynamics). However, as one moves higher in altitude, the variability of IAGOS quickly deviates from the local variability to move closer to the regional-scale variability partly driven by mesoscale meteorology such as frontal passages.
The correlations between O3 hourly time series from IAGOS and AQN urban background stations are strong close to the surface (around 0.85) and decrease with altitude (down to 0.3–0.4 at 4 km ASL). Between IAGOS and GAW stations, the correlation profiles highlight some common features with CO, namely an increase of the correlation with altitude up to a maximum. The altitude of maximum correlation also appears to be related to the station elevation, but the discrepancies between both can be stronger than for CO. For instance, the maximum correlation between IAGOS and SNB (elevation of 3,106 m) is reached at about 1,500 m ASL. The agreement for the AQN rural background station is relatively good (maximum correlation at about 600–700 m ASL for an elevation of 800 m). As for CO, the correlation is higher when considering daily or monthly time series and the results remain qualitatively the same.
Note that when considering only the 12:00–17:00 LT time period, the picture remains the same except that correlations between IAGOS and AQN stations increase to 0.6–0.8 for CO and 0.9 for O3 at the hourly scale (as expected, see Figure 4 and Sect. 3.2). Note also that although some correlations between GAW and IAGOS data are relatively low to moderate for both CO and O3, they remain in the range of the correlations obtained between GAW stations themselves. To illustrate it, for both CO and O3, the correlations between all pairs of GAW stations have been calculated based on hourly time series. They are plotted on Figure 8 (green triangles) as a function of the difference of elevation (in absolute value) between two given GAW stations. Similarly, we also plotted on Figure 8 the correlation between GAW stations and IAGOS observations at each altitude level (i.e. one grey point in Figure 8 represents the correlation between the hourly time series at one given GAW station and the hourly time series of IAGOS data at one given altitude level) against the difference of altitude (i.e. the difference between the elevation of the GAW station and the IAGOS altitude considered). Correlations are usually the lowest for biggest altitude differences, but increase as the difference of altitude gets smaller. At similar altitudes (differences below a few hundreds of metres), the correlations obtained are quite variable but tend to be higher.
We now investigate how trends deduced from IAGOS measurements are comparable with the trends observed at the surface stations. Annual trends calculated by linear regression based on the time series of CO annual averages are shown in Figure 9. Most trends show a statistically significant decrease (at a 95% confidence level) of CO over the period 2002–2012. In agreement with numerous other studies (e.g. Dils et al., 2011; Worden et al., 2013; Petetin et al., 2016a), this decrease over Europe is mainly due to the reduction of CO anthropogenic emissions over the last decades (Yoon and Pozzer, 2014; Strode et al., 2016). The strongest decrease is observed at the traffic stations with best estimates of the trend ranging from –5.5 to –10% yr–1. The urban background stations show lower negative trends, ranging from –2.5 to –6% yr–1. Such differences of CO trends between traffic and urban background stations have already been highlighted in Europe by Guerreiro et al. (2014). Among the GAW stations, 7 stations have a negative trend ranging between –4 and –1% yr–1 (JFJ, SNB, SSL, RIG, PAY, NGL, KMW), while the trends at the 3 other stations are not significant (KVV, HPB, KOS). In the lowest altitude levels, IAGOS data show a significant decrease of CO mixing ratios at the same rate as urban background stations (around –4% yr–1). Contrary to most traffic stations, the difference of trends between IAGOS and urban background stations are usually statistically insignificant. The IAGOS negative trends decrease with altitude, down to –2% yr–1 at 2 km. Such a decrease of CO in the IAGOS dataset of Frankfurt has already been highlighted by Petetin et al. (2016a). Thus, as for the distribution of CO mixing ratios, IAGOS observations progressively shift from a behaviour similar to urban background stations to a behaviour in reasonable agreement with the highest GAW stations, as one moves toward higher altitudes. Quite similar features are observed with seasonal trends (not shown).
All O3 annual trends from IAGOS and the AQN appear statistically not significant (see Figure S-6 in the Supplement). No significant differences between these two datasets are highlighted. Among the GAW stations, 2 stations (KOS and NGL) out of 10 show a significant decrease of O3 over the period 2002–2012, although these trends are not strongly significant (about –1.5 ± 1.2% yr–1). They are mostly driven by a significant decrease in summer and/or autumn. Slightly negative or insignificant trends of O3 in Europe over the 2000s have already been highlighted in other studies (e.g. Cui et al., 2011; Logan et al., 2012; Parrish et al., 2014).
In this section, we further discuss the potential influence of the airport pollution on the IAGOS measurements. One characteristic of the IAGOS data is that profiles can be obtained during either ascent (take-off) or descent (landing) phases. Although there are exceptions (see Figure S-7 in the Supplement for a plot of the aircraft orientation as a function of the wind direction for all concomitant flights at Frankfurt), the general rule is to take-off and land against the wind when possible, which helps slowing down the aircraft during the landing and increasing the lift on the wings during the take-off. Such operations are facilitated by the fact that runways are preferably built following the local dominant wind directions. For instance, the runways available at the Frankfurt airport offer four possible orientations for take-offs and landings: ENE, WSW, S, N (where N, S, E, W stand for North, South, East, West). Depending on the wind direction and the configuration of both the runways and the different airport facilities, and assuming an influence of the airport pollution on the IAGOS measurements, we might expect a difference of O3 or CO mixing ratios during landing and take-offs. In particular, we might expect higher CO mixing ratios during the landing phase (when the wind blows the airport plume toward the aircraft) than during the take-off phase (when the aircraft get further from the airport with a headwind clear from any influence of airport emissions). Conversely, as O3 is quickly titrated by the NO emissions, we might expect lower O3 mixing ratios during the landing than during the take-off, although some O3 local production may lead to a more complex and ambiguous picture.
To investigate this point, we compared the O3 and CO IAGOS profiles during these two phases over the period 2002–2012. We selected at Frankfurt all concomitant landings and take-offs profiles over a time window of 30 min. The mean profiles are shown in Figure 10, with their corresponding uncertainties at a 95% confidence level (i.e. ±2 standard deviations normalized by the square root of the number of points). Contrary to what would have been expected if IAGOS data were more influenced by the airport pollution during landings, the CO mixing ratios are slightly higher during take-offs. Results show statistically insignificant biases of about 5% below 300 m ASL and (slightly) significant biases of about 10% between 300 and 900 m ASL, the strongest difference (15%) being found at 350–400 m ASL. Above 900 m ASL, the differences are much lower and remain insignificant. The agreement between landings and take-offs is very good for O3 with a mean insignificant difference below 1% over the first kilometre.
If the airport emissions were influencing IAGOS data, one would expect higher CO mixing ratios during landing, especially close to the surface, which is not the case here. The differences previously highlighted may be at least partly explained by the spatial heterogeneity of the CO mixing ratios field in the boundary layer around Frankfurt. At low altitudes (below 300 m ASL), both the ascending and descending aircraft are closer to each other, leading to small (and insignificant) differences of CO mixing ratio. Higher in altitude between 300 and 900 m ASL, the horizontal distance between the two aircraft quickly increases (reaching typically 5–20 km) since they are often flying in the same direction (close to the wind direction). Considering the strongly heterogeneous spatial distribution of emission sources in the region of Frankfurt (patchwork of forests, urban and agricultural areas), this may explain a part of the differences between landings and take-offs. Note that take-off and landing observations are not similarly distributed around Frankfurt notably since the runway oriented S-N is only used for take-offs. If we go further in altitude (above 1 km ASL), the aircraft typically reaches the free troposphere where CO mixing ratio fields are more homogeneous. Conversely, the very low differences of O3 found between landings and take-offs may be due to the fact, as a secondary pollutant, the O3 fields are more homogeneous (relatively to CO).
Note that comparing daily or monthly averages based on all available data (rather than averaging only simultaneous landing and take-off data), stronger differences are found due to the fact that (i) both O3 and CO depict a substantial diurnal variability in the lower troposphere, and (ii) landings and take-offs are not similarly distributed over the day in the IAGOS database (landings are more numerous during the morning while take-offs are more equally distributed along daytime).
In the previous sections, we highlighted that the O3 and CO mixing ratios typically measured by IAGOS aircraft in the first altitude levels at Frankfurt are close to the mixing ratio measured at urban background stations. Higher in altitude, they come closer to the mixing ratios observed at the regional scale by the GAW network. The progressive shift from a behaviour typical of urban background stations to a behaviour closer to the regional background was also highlighted on the temporal variability of O3 and CO. These results are valid for Frankfurt, but the question arises of whether they can be generalized to other IAGOS airports. Compared with Frankfurt, IAGOS data are much sparser at other airports, which limits our ability to conduct similar in-depth analysis. However, some general comparisons can still be performed at few other airports in order to assess how far these previous results may change at other locations. In this section, we thus extend the previous analysis to two other airports of West-Central Europe: Vienna and Paris. The analysis is restricted to a comparison of the overall distribution of mixing ratios and a discussion on the correlation of hourly and daily datasets. For information purposes, the corresponding figures are given in the Supplement (Figures S-8 to S-10 for Vienna, Figures S-11 to S-13 for Paris). To facilitate comparisons among airports, the mean CO and O3 mixing ratios at the different surface stations and in altitude are reported in Table 2 for the 3 cities.
|Species||Airport||Rural background mean ± stdev (min–maxa)||Urban background mean ± stdev (min–maxa)||Traffic mean (min–maxa)||IAGOS
|1st level||2nd level||3rd level||4th level|
|CO||Frankfurt||–||348 ± 212
|630 ± 414
|292 ± 142||261 ± 124||244 ± 109||230 ± 104|
|Vienna||–||272 ± 163
|439 ± 268
|347 ± 152b||271 ± 126||222 ± 104||213 ± 96|
|Paris||–||486 ± 264
|1,322 ± 652
|275 ± 168||242 ± 123||218 ± 93||207 ± 78|
|O3||Frankfurt||35 ± 15
|19 ± 17
|–||17 ± 16||20 ± 17||20 ± 16||21 ± 16|
|Vienna||35 ± 19
|33 ± 19
|–||21 ± 13b||26 ± 16||32 ± 19||35 ± 19|
|Paris||28 ± 19
|22 ± 19
|–||19 ± 16||20 ± 16||21 ± 16||23 ± 16|
The comparison between IAGOS and surface CO measurements in Vienna gives quite similar results as in Frankfurt. IAGOS data in Vienna are available only between 2002 and 2006. Considering only the days with available IAGOS data at one altitude level at least, the mean CO mixing ratio are lower than at Frankfurt, with 439 ± 268 and 272 ± 163 ppbv at traffic and urban background stations, respectively. Although it lies between these two values, the mean CO mixing ratio measured by IAGOS in the first altitude level (0–50 m ASL) is quite strong (347 ± 152 ppbv) compared to Frankfurt. However, this value is not fully representative as it is based on only 236 points (compared to more than 2,000 for altitude levels above 100 m) and more importantly, without any data during summertime (i.e. when CO is minimum). As mentioned in Sect. 2.1, this study is using the barometric altitude estimated from the temperature and the pressure measured by the aircraft assuming standard conditions at the surface. This can lead to barometric altitudes below the actual airport elevation (180 m for Vienna) under specific atmospheric conditions characterized by low pressure (cyclone) and/or low temperature. Such conditions are mostly encountered in winter and not in summer, which explains the absence of IAGOS data at this first altitude level in summer. In addition, these cyclonic conditions may be associated to stronger local CO emissions (for instance, a wintertime cold snap increases the need for residential heating). At the next levels, the CO mixing ratios measured by IAGOS at Vienna are in better agreement with results obtained at Frankfurt.
It is worth noting that exact differences between IAGOS and urban background stations cannot be calculated from the figures in Table 2 as the mean urban background at the surface (here calculated from all hours with at least one IAGOS observation between 0 and 4 km ASL, see Sect. 2.3) changes if we consider the IAGOS availability at one specific altitude level. Exact comparisons between all individual hourly surface data with concomitant IAGOS data at the corresponding altitudes (i.e. the elevation of the station) were performed, and results are reported in Table 3 (results concerning Frankfurt have been already discussed in the previous sections). On average, the CO measured by IAGOS aircraft is 48 and 17% lower than at surface traffic and urban background stations, respectively, which remains in agreement with the results at Frankfurt (–61 and –26%, respectively).
|Species||Airport||Rural background stations||Urban background stations||Traffic stations|
For O3, the mean mixing ratios are 33 ± 19 and 35 ± 19 ppbv at urban and rural background stations, respectively. Compared to Frankfurt, IAGOS data at Vienna show lower O3 mixing ratios in the first levels, but the agreement is good higher in altitude (mean difference below 3 ppbv above 400 m ASL), in agreement with the results of Logan et al. (2012) in the low/middle troposphere (2.6–5 km). Considering exact comparisons between IAGOS and surface stations, the mean difference is only +2 and +10% for rural and urban background stations, respectively (Table 3). As for Frankfurt, these differences show diurnal variations with highest biases during the morning and lowest during the second half of the day (not shown). The correlation between the two datasets is strong (r = 0.82).
Therefore, for both CO and O3, IAGOS aircraft at Vienna measure mixing ratios in agreement with the urban background observed at the surface by the close-by AQ monitoring stations. Despite a lower number of observations available, the correlation profiles of CO at Vienna (Figure S-10 in the Supplement) are also in good agreement with those obtained at Frankfurt. For O3, quite similar correlations are found in both cities, but some differences are found in the shape of profiles. Strongest close to the surface, the correlations between IAGOS and AQN stations are found to decrease more slowly and more uniformly over the first 4 kilometres (while the decrease of correlation at Frankfurt was occurring mainly in the first kilometre). They usually remain similar or slightly higher than the correlations between IAGOS and GAW stations.
At Paris, we combine the measurements of both Charles-de-Gaulle and Orly airports (most data are obtained at the former airport). The observed pollution from CO is much stronger than in the other two cities, with 486 ± 264 ppbv at urban background stations and 1,322 ± 652 ppbv at traffic stations on average. These numbers are biased high as they are calculated based on a limited number of points with concomitant IAGOS observations, all during the beginning of the period (2002–2005). Independently of IAGOS, the negative trends in CO observed between 2002 and 2012 at the urban background stations in Paris (not shown) are higher than at the two other airports (about –7% yr–1, against less than –5% yr–1 at other airports), leading to a mean CO over the period 2002–2012 reduced to 294 ± 209 ppbv. This is also the case for traffic stations (trends ranging from –8 to –12% yr–1, against less than –8% yr–1 at other airports) except that the mean CO over 2002–2012 is still higher than at the other airports (881 ± 585 ppbv).
The mixing ratios measured at Paris by IAGOS aircraft are much lower than at urban background stations. The mean urban background of CO is calculated based on only two stations, including one in the centre of Paris (PA1H_U: Paris 1st district) and the another one (AUB_U: Aubervilliers) in the adjacent suburbs (350 m from the Paris ring road highway). On average, the relative difference between IAGOS and these urban background stations is –48% (Table 3), thus much stronger than at Frankfurt or Vienna. Although the number of data points is a lot lower than at the two other airports (228 data, against 1,384 and 28,976 for Vienna and Frankfurt, respectively), the difference is statistically significant. Based on more numerous data, the difference between IAGOS and traffic stations remains higher than at other airports (–82% on average). For both types of station, the correlation is also much lower (0.38 and 0.21, respectively). The poor agreement can be at least partly explained by the IAGOS data availability predominantly in the morning hours (55% of the 236 points are between 07:00–10:00 LT, 74% between 06:00–11:00 LT). As mentioned in Sect. 3.2, the difference between IAGOS observations and surface observations at urban background stations varies diurnally, with larger biases during the morning rush hours. A similar behaviour is observed at Paris (not shown), although IAGOS CO mixing ratios remain substantially lower than at urban background stations.
Compared with CO, there are many more data from stations measuring O3 in/around Paris (8 rural background stations, 21 urban background stations) available. They show mean O3 mixing ratios of 28 ± 19 and 22 ± 19 ppbv at the rural and urban background stations, respectively. The IAGOS data show slightly lower O3 mixing ratios, with mean differences of –22 and –11% for rural and urban background stations (Table 3). Similarly to Frankfurt and Vienna, both are well correlated (r > 0.7).
The bias of O3 between IAGOS and rural background stations can be greatly reduced by restricting the dataset to days with windy conditions. This is clearly illustrated in Figure 11 in which the relative bias is shown for different values of minimum wind speed from 0 to 10 m s–1. This bias progressively decreases when data associated with low wind speed (measured by IAGOS aircraft) are removed: applying a minimum wind speed of 2, 4, 6, 8 and 10 m s–1 leads to a bias of –21, –16, –14, –11 and –10%, respectively. For wind criteria above 8 m s–1, biases are not significant. However, such restrictions of the dataset slightly reduce the correlations. Such an influence of the wind was not observed at the other airports. A good agreement between IAGOS and rural background stations is not expected under very low wind conditions, as mixing in the vicinity of the surface station is reduced. However, the persistent decrease of the bias for higher wind speed was not expected. It may be due to the flat orography of the Paris region that favours homogenisation of the spatial O3 distribution at a regional scale when the wind is sufficiently high (contrary to Frankfurt and Vienna where the surrounding orography is more complex). Note also that a similar reduction of the bias with the wind speed is highlighted between IAGOS and the EIFF3_U station located at the 3rd floor of the Eiffel tower (315 m ASL).
The CO and O3 mixing ratios measured by IAGOS at different altitude levels in the lower troposphere around three European airports have been compared with surface measurements available from local air quality monitoring networks (within 50–80 km from the airport) and regional GAW stations (within 500 km from the airport). A focus was made on Frankfurt airport where the IAGOS data record is the densest and longest. At Frankfurt, the measurements at (urban) traffic stations show a very specific behaviour, with very high CO mixing ratios, and a strong negative trend over the period 2002–2012. Conversely, the CO and O3 measured at urban background stations were found to share common characteristics with the CO and O3 measured by IAGOS in the altitude levels closest to the surface, in terms of distribution, seasonal variations and trends (Figures 3, 6, 9). IAGOS data showed slightly lower CO and slightly higher O3, which suggests a smaller influence of local emission sources than at urban background stations. These differences exhibit a diurnal variation with largest biases during the morning rush hours when the local traffic emissions increase the CO mixing ratios at both urban background and traffic stations (Figure 4). In addition, the CO and O3 mixing ratios measured at the nearby surface stations appeared reasonably well correlated with the IAGOS airborne data at the lowest altitude levels (r ~ 0.6–0.7 at the daily scale, 0.7–0.8 at the monthly scale) (Figure 7). At higher altitudes, these characteristics of the IAGOS observations quickly deviate from the urban background and approach the regional background observed by the different GAW surface stations located in and around Germany. This is demonstrated by the fact that the correlation between IAGOS and GAW datasets increases with altitude, with maximum correlations mostly obtained at an altitude close to the elevation of the surface station (Figure 6). The correlation between IAGOS and GAW stations is in the same range as the correlation among the GAW stations themselves (Figure 8). The vertical distribution of CO and O3 derived from the IAGOS airborne measurements was found to be in close agreement with the vertical distribution deduced in the first 4 km from the GAW stations at different elevations (Figure 5). A comparison between concomitant ascent and descent profiles at Frankfurt have shown a good agreement (insignificant bias) on CO below 300 m ASL and above 1,000 m ASL but some small significant differences between 300 and 1,000 m ASL, with lower CO during landings (Figure 10). The agreement on O3 was very good whatever the altitude. Despite sparser IAGOS data, some comparisons were extended to Vienna and Paris airports. In both cities, the CO mixing ratios measured by IAGOS in the first altitude levels are always lower than the urban background given measured at the surface. At Vienna, the agreement with Frankfurt is good, as illustrated by a mean difference of CO between IAGOS and urban background stations of –17% on average (against –26% at Frankfurt). At Paris, much lower CO mixing ratios are measured by IAGOS (difference of –46%), at least partly due to a high proportion of data during the morning, when higher biases were also observed at Frankfurt and Vienna. With biases below ±12%, the agreement of O3 between IAGOS and urban background stations appears very satisfactory at all 3 airports. Although some quantitative differences may exist, the results at Vienna and Paris remain reasonably consistent with the results obtained at Frankfurt.
Therefore, several important conclusions can be drawn at these airports. Firstly, the IAGOS observations close to the surface do not appear to be strongly influenced by local emissions from either the airport activities on the tarmac or the other aircraft sharing nearby flight tracks. Secondly, the comparison with the surrounding surface stations from the local AQN indicates that the IAGOS observations in the first few hundreds meters above the surface have a representativeness typical of urban or more precisely suburban background stations where the three airports are located. Thirdly, the comparison with (more distant) regional background stations from the GAW network shows that as one moves higher in altitude, the IAGOS observations shift toward a regional representativeness. The boundary of transition between these two variability regimes likely depends on the local meteorological conditions, and in particular the PBL height and state. The transition may thus be more abrupt than our results suggest since in this study, numerous profiles of different PBL height are combined, which automatically smoothes the features that may exist at the transition between PBL and lower free troposphere. The good consistency between GAW and IAGOS observations at the different altitudes (more particularly above the first 500 m) gives confidence on the ability of IAGOS data to measure a reliable vertical distribution of the pollutants in the lower troposphere.
Several reasons can explain the absence of strong influence of the local emissions from the airport activities and/or other aircraft. First, although CO mixing ratios as high as a few ppmv can typically be reported in international airports (e.g. Yu et al., 2004; Schürmann et al., 2007), the IAGOS system is designed to start measurements when the wheels of the aircraft leave the ground during ascents (or when they touch down during descents). At this moment, the aircraft is already moving at a high speed (typically 50 m s–1) and is thus expected to quickly get away from the local emissions associated with the airport activities. A standard landing and take-off (LTO) cycle as defined by the International Civil Aviation Organization (ICAO) includes 4 phases with different durations and percentages of thrust: the approach phase (30% thrust, 4 min), the idle(-taxi) phase (7% thrust, 26 min), the take-off phase (100%, 0.7 min) and the climb phase (85% thrust, 2.2 min) (Masiol and Harrison, 2014). IAGOS measurements thus start at the beginning of the climb phase for ascents, and at the end of the approach phase for descents. The emission factors of CO are much higher during the idle phase than during the other phases (see Masiol and Harrison, 2014 for a review). This is due to a less complete combustion associated with cold combustor temperatures in the aircraft engines (Herndon et al., 2008). However, IAGOS is not measuring during this phase, which likely explains the absence (or the very low frequency of occurrence) of strong CO peaks: indeed, between 0 and 250 m ASL at Frankfurt, the maximum CO mixing ratio is 2,358 ppbv, and the 99.9th percentile of all hourly mixing ratios is only 1,095 ppbv. Secondly, in order to reduce the risk of collision and/or the exposure to the wake vortex turbulence caused by other aircraft, several separation standards are fixed by the ICAO. For instance, the vertical separation minimum between two aircraft is fixed to 300 m (1,000 ft) below ~8.8 km of altitude (and the double above) (ICAO, 2016). In addition, although the minimum duration between two consecutive takeoffs/landings can be as short as a few minutes (it varies depending on the aircraft and the airport), commercial aircraft are not allowed to follow each other too closely on the same track. Considering the fact that the dispersion of pollutants is more efficient at altitude (stronger wind, absence of re-circulation loops caused by buildings and/or canyon streets), these different separation standards appear sufficient to avoid measuring directly the exhausts from other aircraft. Detailed studies on airport air quality aspects with IAGOS data are subject of on-going work.
Therefore, this study shows that IAGOS can be seen as a complement of surface stations to monitor the air quality in/around the agglomeration. Although sporadic in time, IAGOS data provide useful information on the vertical distribution of pollution in the boundary layer. The spatial representativeness of the IAGOS observations in the lower troposphere appears large enough to offer a new opportunity to validate models and satellites in the PBL, in complement to surface stations and ozonesondes. The importance of improving models on the vertical dimension has been already underlined in several studies (Solazzo et al., 2013; and references therein). Besides, this has recently justified the use of IAGOS to validate operationally the CAMS regional chemistry-transport models in Europe (see http://www.iagos.fr/cams for daily comparisons). This study confirms that such comparisons are entirely relevant. In addition, IAGOS offers the major advantage of providing observations in many large cities with the same instrumental system, thus ensuring a consistency between all the measurements. This is particularly interesting for comparing the air quality in cities from different countries that may not use comparable instruments and standard scales at the surface stations.
It is worth remembering that these results are based on a limited set of airports. In particular, the most in-depth analysis was restricted to Frankfurt airport where the IAGOS data are the most numerous. Considering the potentially large differences of environment from one airport to the other (e.g. intensity of the local air traffic, distance from the agglomeration, size of the agglomeration and intensity of local emissions, orography, local meteorology), they may not be valid for all airports visited by IAGOS aircraft since 1994 (~290). This study thus has to be considered as a first step, and should be extended in the future as larger amounts of data become available around the different airports, in particular in highly polluted Asian megacities.
No new measurements were made for this review article. All datasets mentioned in the text were obtained from existing databases. The IAGOS data are available on: http://www.iagos.fr, the AIRBASE data (for Frankfurt and Vienna) on: https://www.eea.europa.eu/data-and-maps/data/airbase-the-european-air-quality-database-7, the AIRPARIF data (for Paris) on: https://www.airparif.asso.fr. The GAW data are taken from the World Data Centre for Greenhouse Gases (WDCGG) http://ds.data.jma.go.jp/gmd/wdcgg/.
The supplemental files for this article can be found as follows:
The authors acknowledge the strong support of the European Commission, Airbus, and the Airlines (Lufthansa, Air-France, Austrian, Air Namibia, Cathay Pacific, Iberia, China Airlines, Hawaiian Airlines so far) who carry the MOZAIC or IAGOS equipment and perform the maintenance since 1994. In its last 10 years of operation, MOZAIC has been funded by INSU-CNRS (France), Météo-France, Université Paul Sabatier (Toulouse, France) and Research Center Jülich (FZJ, Jülich, Germany). IAGOS has been additionally funded by the EU projects IAGOS-DS and IAGOS-ERI. The MOZAIC-IAGOS database is supported by AERIS (CNES and INSU-CNRS). Data are also available via AERIS web site www.aeris-data.fr. We also acknowledge AIRPARIF for providing freely air pollution data in the Paris region. Ozone and CO mixing ratios at GAW stations in Europe were provided by the World Data Centre for Greenhouse Gases (WDCGG), in cooperation with the Japan Meteorological Agency and the World Meteorological Organisation (WMO). In particular, we acknowledge: the Empa (Swiss Federal Institute for Materials Science and Technology) for GAW data at Jungfraujoch, Payerne and Rigi; the UBA (Umwelt Bundesamt, the German Federal Environment Agency) for GAW data at Neuglobsow and Schauinsland; the DWD (Deutscher Wetterdienst) for GAW data at Hohenpeissenberg; the CHMI (Czech HydroMeteorological Institute) for GAW data at Kosetice; the EAA (Environmental Agency Austria) for the GAW data at Sonnblick; the RIVM (Dutch National Institute for public Health and the Environment) for GAW data at Kollumerwaard, the ARSO (Environmental Agency of the Republic of Slovenia) for GAW data at Krvavec. We also thank the two anonymous reviewers for their valuable contribution to this paper.
The authors have no competing interests to declare.
Brenninkmeijer, CAM, Crutzen, P, Boumard, F, Dauer, T, Dix, B, Ebinghaus, R, Filippi, D, Fischer, H, Franke, H, Frieβ, U, Heintzenberg, J, Helleis, F, Hermann, M, Kock, HH, Koeppel, C, Lelieveld, J, Leuenberger, M, Martinsson, BG, Miemczyk, S, Moret, HP, Nguyen, HN, Nyfeler, P, Oram, D, O’Sullivan, D, Penkett, S, Platt, U, Pupek, M, Ramonet, M, Randa, B, Reichelt, M, Rhee, TS, Rohwer, J, Rosenfeld, K, Scharffe, D, Schlager, H, Schumann, U, Slemr, F, Sprung, D, Stock, P, Thaler, R, Valentino, F, van Velthoven, P, Waibel, A, Wandel, A, Waschitschek, K, Wiedensohler, A, Xueref-Remy, I, Zahn, A, Zech, U and Ziereis, H 2007 Civil Aircraft for the regular investigation of the atmosphere based on an instrumented container: The new CARIBIC system. Atmos. Chem. Phys 7(18): 4953–4976. DOI: 10.5194/acp-7-4953-2007
Bundke, U, Berg, M, Houben, N, Ibrahim, A, Fiebig, M, Tettich, F, Klaus, C, Franke, H and Petzold, A 2015 The IAGOS-CORE aerosol package: Instrument design, operation and performance for continuous measurement aboard in-service aircraft. Tellus B Chem. Phys. Meteorol 67(1): 28339. DOI: 10.3402/tellusb.v67.28339
Chevalier, A, Gheusi, F, Delmas, R, Ordóñez, C, Sarrat, C, Zbinden, R, Thouret, V, Athier, G and Cousin, J-M 2007 Influence of altitude on ozone levels and variability in the lower troposphere: A ground-based study for western Europe over the period 2001–2004. Atmos. Chem. Phys 7(16): 4311–4326. DOI: 10.5194/acp-7-4311-2007
Clerbaux, C, George, M, Turquety, S, Walker, KA, Barret, B, Bernath, P, Boone, C, Borsdorff, T, Cammas, JP, Catoire, V, Coffey, M, Coheur, P-F, Deeter, M, De Mazière, M, Drummond, J, Duchatelet, P, Dupuy, E, de Zafra, R, Eddounia, F, Edwards, DP, Emmons, L, Funke, B, Gille, J, Griffith, DWT, Hannigan, J, Hase, F, Höpfner, M, Jones, N, Kagawa, A, Kasai, Y, Kramer, I, Le Flochmoën, E, Livesey, NJ, López-Puertas, M, Luo, M, Mahieu, E, Murtagh, D, Nédélec, P, Pazmino, A, Pumphrey, H, Ricaud, P, Rinsland, CP, Robert, C, Schneider, M, Senten, C, Stiller, G, Strandberg, A, Strong, K, Sussmann, R, Thouret, V, Urban, J and Wiacek, A 2008 CO measurements from the ACE-FTS satellite instrument: Data analysis and validation using ground-based, airborne and spaceborne observations. Atmos. Chem. Phys 8(9): 2569–2594. DOI: 10.5194/acp-8-2569-2008
Cui, J, Pandey Deolal, S, Sprenger, M, Henne, S, Staehelin, J, Steinbacher, M and Nédélec, P 2011 Free tropospheric ozone changes over Europe as observed at Jungfraujoch (1990–2008): An analysis based on backward trajectories. J. Geophys. Res 116(D10): 304. DOI: 10.1029/2010JD015154
Dils, B, Cui, J, Henne, S, Mahieu, E, Steinbacher, M and De Mazière, M 2011 1997–2007 CO trend at the high Alpine site Jungfraujoch: A comparison between NDIR surface in situ and FTIR remote sensing observations. Atmos. Chem. Phys 11(13). DOI: 10.5194/acp-11-6735-2011
Ding, AJ, Wang, T, Thouret, V, Cammas, J-P and Nédélec, P 2008 Tropospheric ozone climatology over Beijing: Analysis of aircraft data from the MOZAIC program. Atmos. Chem. Phys 8(1): 1–13. DOI: 10.5194/acp-8-1-2008
Elguindi, N, Clark, H, Ordóñez, C, Thouret, V, Flemming, J, Stein, O, Huijnen, V, Moinat, P, Inness, A, Peuch, V-H, Stohl, A, Turquety, S, Athier, G, Cammas, J-P and Schultz, M 2010 Current status of the ability of the GEMS/MACC models to reproduce the tropospheric CO vertical distribution as measured by MOZAIC. Geosci. Model Dev 3(2): 501–518. DOI: 10.5194/gmd-3-501-2010
Emmons, LK, Edwards, DP, Deeter, MN, Gille, JC, Campos, T, Nédélec, P, Novelli, P and Sachse, G 2009 Measurements of Pollution In The Troposphere (MOPITT) validation through 2006, Atmos. Chem. Phys 9(5): 1795–1803. DOI: 10.5194/acp-9-1795-2009
Filges, A, Gerbig, C, Chen, H, Franke, H, Klaus, C and Jordan, A 2015 The IAGOS-core greenhouse gas package: A measurement system for continuous airborne observations of CO2, CH4, H2O and CO. Tellus B Chem. Phys. Meteorol 67(1): 27989. DOI: 10.3402/tellusb.v67.27989
Guerreiro, CBB, Foltescu, V and de Leeuw, F 2014 Air quality status and trends in Europe. Atmos. Environ 98: 376–384. DOI: 10.1016/j.atmosenv.2014.09.017
Heald, CL, Jacob, DJ, Fiore, AM, Emmons, LK, Gille, JC, Deeter, MN, Warner, J, Edwards, DP, Crawford, JH, Hamlin, AJ, Sachse, GW, Browell, EV, Avery, MA, Vay, SA, Westberg, DJ, Blake, DR, Singh, HB, Sandholm, ST, Talbot, RW and Fuelberg, HE 2003 Asian outflow and trans-Pacific transport of carbon monoxide and ozone pollution: An integrated satellite, aircraft, and model perspective. J. Geophys. Res. Atmos 108(D24): n/a–n/a. DOI: 10.1029/2003JD003507
Herndon, SC, Jayne, JT, Lobo, P, Onasch, TB, Fleming, G, Hagen, DE, Whitefield, PD and Miake-Lye, RC 2008 Commercial Aircraft Engine Emissions Characterization of in-Use Aircraft at Hartsfield-Jackson Atlanta International Airport. Environ. Sci. Technol 42(6): 1877–1883. DOI: 10.1021/es072029+
ICAO 2016 Doc 4444 – Procedures for Air Navigation Services: Air Traffic Management, 16th edition. [online] Available from: http://flightservicebureau.org/wp-content/uploads/2017/03/ICAO-Doc4444-Pans-Atm-16thEdition-2016-OPSGROUP.pdf.
Kalabokas, PD, Cammas, J-P, Thouret, V, Volz-Thomas, A, Boulanger, D and Repapis, CC 2013 Examination of the atmospheric conditions associated with high and low summer ozone levels in the lower troposphere over the eastern Mediterranean. Atmos. Chem. Phys 13(20): 10339–10352. DOI: 10.5194/acp-13-10339-2013
Kalabokas, PD, Volz-Thomas, A, Brioude, J, Thouret, V, Cammas, J-P and Repapis, CC 2007 Vertical ozone measurements in the troposphere over the Eastern Mediterranean and comparison with Central Europe. Atmos. Chem. Phys 7(14): 3783–3790. DOI: 10.5194/acp-7-3783-2007
Liu, G, Tarasick, DW, Fioletov, VE, Sioris, CE and Rochon, YJ 2009 Ozone correlation lengths and measurement uncertainties from analysis of historical ozonesonde data in North America and Europe. J. Geophys. Res 114(D4). DOI: 10.1029/2008JD010576
Liu, H, Jacob, DJ, Bey, I, Yantosca, RM, Duncan, BN and Sachse, WG 2003 Transport pathways for Asian pollution outflow over the Pacific: Interannual and seasonal variations. J. Geophys. Res 108(D20): 8786. DOI: 10.1029/2002JD003102
Logan, JA, Staehelin, J, Megretskaia, IA, Cammas, J-P, Thouret, V, Claude, H, De Backer, H, Steinbacher, M, Scheel, H-E, Stübi, R, Fröhlich, M and Derwent, R 2012 Changes in ozone over Europe: Analysis of ozone measurements from sondes, regular aircraft (MOZAIC) and alpine surface sites. J. Geophys. Res 117(D9): 301. DOI: 10.1029/2011JD016952
Machida, T, Matsueda, H, Sawa, Y, Nakagawa, Y, Hirotani, K, Kondo, N, Goto, K, Nakazawa, T, Ishikawa, K and Ogawa, T 2008 Worldwide Measurements of Atmospheric CO2 and Other Trace Gas Species Using Commercial Airlines. J. Atmos. Ocean. Technol 25(10): 1744–1754. DOI: 10.1175/2008JTECHA1082.1
Marenco, A, Thouret, V, Nédélec, P, Smit, H, Helten, M, Kley, D, Karcher, F, Simon, P, Law, K, Pyle, J, Poschmann, G, Von Wrede, R, Hume, C and Cook, T 1998 Measurement of ozone and water vapor by Airbus in-service aircraft: The MOZAIC airborne program, an overview. J. Geophys. Res. Atmos 103(D19): 25631–25642. DOI: 10.1029/98JD00977
Masiol, M and Harrison, RM 2014 Aircraft engine exhaust emissions and other airport-related contributions to ambient air pollution: A review. Atmos. Environ 95: 409–455. DOI: 10.1016/j.atmosenv.2014.05.070
Monks, PS, Archibald, AT, Colette, A, Cooper, O, Coyle, M, Derwent, R, Fowler, D, Granier, C, Law, KS, Mills, GE, Stevenson, DS, Tarasova, O, Thouret, V, von Schneidemesser, E, Sommariva, R, Wild, O and Williams, ML 2015 Tropospheric ozone and its precursors from the urban to the global scale from air quality to short-lived climate forcer. Atmos. Chem. Phys 15(15): 8889–8973. DOI: 10.5194/acp-15-8889-2015
Nédélec, P, Blot, R, Boulanger, D, Athier, G, Cousin, J-M, Gautron, B, Petzold, A, Volz-Thomas, A and Thouret, V 2015 Instrumentation on commercial aircraft for monitoring the atmospheric composition on a global scale: The IAGOS system, technical overview of ozone and carbon monoxide measurements. Tellus B 67: 1–16. DOI: 10.3402/tellusb.v67.27791
Nédélec, P, Cammas, J-P, Thouret, V, Athier, G, Cousin, J-M, Legrand, C, Abonnel, C, Lecoeur, F, Cayez, G and Marizy, C 2003 An improved infrared carbon monoxide analyser for routine measurements aboard commercial Airbus aircraft: Technical validation and first scientific results of the MOZAIC III programme. Atmos. Chem. Phys 3(5): 1551–1564. DOI: 10.5194/acp-3-1551-2003
Parrish, DD, Lamarque, J-F, Naik, V, Horowitz, L, Shindell, DT, Staehelin, J, Derwent, R, Cooper, OR, Tanimoto, H, Volz-Thomas, A, Gilge, S, Scheel, H-E, Steinbacher, M and Fröhlich, M 2014 Long-term changes in lower tropospheric baseline ozone concentrations: Comparing chemistry-climate models and observations at northern midlatitudes. J. Geophys. Res. Atmos 119(9): 5719–5736. DOI: 10.1002/2013JD021435
Parrish, DD, Law, KS, Staehelin, J, Derwent, R, Cooper, OR, Tanimoto, H, Volz-Thomas, A, Gilge, S, Scheel, H-E, Steinbacher, M and Chan, E 2013 Lower tropospheric ozone at northern midlatitudes: Changing seasonal cycle. Geophys. Res. Lett 40(8): 1631–1636. DOI: 10.1002/grl.50303
Petetin, H, Thouret, V, Athier, G, Blot, R, Boulanger, D, Cousin, J-M, Gaudel, A, Nédélec, P and Cooper, O 2016b Diurnal cycle of ozone throughout the troposphere over Frankfurt as measured by MOZAIC-IAGOS commercial aircraft. Elem. Sci. Anthr 4(129): 1–11. DOI: 10.12952/journal.elementa.000129
Petetin, H, Thouret, V, Fontaine, A, Sauvage, B, Athier, G, Blot, R, Boulanger, D, Cousin, J-M and Nédélec, P 2016a Characterising tropospheric O3 and CO around Frankfurt over the period 1994–2012 based on MOZAIC–IAGOS aircraft measurements. Atmos. Chem. Phys 16(23): 15147–15163. DOI: 10.5194/acp-16-15147-2016
Petzold, A, Thouret, V, Gerbig, C, Zahn, A, Brenninkmeijer, CAM, Gallagher, M, Hermann, M, Pontaud, M, Ziereis, H, Boulanger, D, Marshall, J, Nédélec, P, Smit, HGJ, Friess, U, Flaud, J-M, Wahner, A, Cammas, J-P and Volz-Thomas, A 2015 Global-scale atmosphere monitoring by in-service aircraft – current achievements and future prospects of the European Research Infrastructure IAGOS. Tellus B Chem. Phys. Meteorol 67(1): 28452. DOI: 10.3402/tellusb.v67.28452
Sahu, LK, Sheel, V, Kajino, M, Deushi, M, Gunthe, SS, Sinha, PR, Sauvage, B, Thouret, V and Smit, HG 2014 Seasonal and interannual variability of tropospheric ozone over an urban site in India: A study based on MOZAIC and CCM vertical profiles over Hyderabad. J. Geophys. Res. Atmos 119(6): 3615–3641. DOI: 10.1002/2013JD021215
Sauvage, B, Thouret, V, Cammas, J-P, Gheusi, F, Athier, G and Nédélec, P 2005 Tropospheric ozone over Equatorial Africa: Regional aspects from the MOZAIC data. Atmos. Chem. Phys 5(2): 311–335. DOI: 10.5194/acp-5-311-2005
Schultz, MG, Akimoto, H, Bottenheim, J, Buchmann, B, Galbally, IE, Gilge, S, Helmig, D, Koide, H, Lewis, AC, Novelli, PC, Plass-Dülmer, C, Ryerson, TB, Steinbacher, M, Steinbrecher, R, Tarasova, O, Tørseth, K, Thouret, V and Zellweger, C 2015 The Global Atmosphere Watch reactive gases measurement network. Elem Sci Anth 3. DOI: 10.12952/journal.elementa.000067
Schürmann, G, Schäfer, K, Jahn, C, Hoffmann, H, Bauerfeind, M, Fleuti, E and Rappenglück, B 2007 The impact of NOx, CO and VOC emissions on the air quality of Zurich airport. Atmos. Environ 41(1): 103–118. DOI: 10.1016/j.atmosenv.2006.07.030
Sheel, V, Bisht, JSH, Sahu, L and Thouret, V 2016 Spatio-temporal variability of CO and O3 in Hyderabad (17°N, 78°E), central India, based on MOZAIC and TES observations and WRF-Chem and MOZART-4 models. Tellus B 68: 30545. DOI: 10.3402/tellusb.v68.30545
Solazzo, E, Bianconi, R, Pirovano, G, Moran, MD, Vautard, R, Hogrefe, C, Appel, KW, Matthias, V, Grossi, P, Bessagnet, B, Brandt, J, Chemel, C, Christensen, JH, Forkel, R, Francis, XV, Hansen, AB, McKeen, S, Nopmongcol, U, Prank, M, Sartelet, KN, Segers, A, Silver, JD, Yarwood, G, Werhahn, J, Zhang, J, Rao, ST and Galmarini, S 2013 Evaluating the capability of regional-scale air quality models to capture the vertical distribution of pollutants. Geosci. Model Dev 6(3): 791–818. DOI: 10.5194/gmd-6-791-2013
Staufer, J, Staehelin, J, Stübi, R, Peter, T, Tummon, F and Thouret, V 2013 Trajectory matching of ozonesondes and MOZAIC measurements in the UTLS – Part 1: Method description and application at Payerne, Switzerland. Atmos. Meas. Tech 6(12): 3393–3406. DOI: 10.5194/amt-6-3393-2013
Staufer, J, Staehelin, J, Stübi, R, Peter, T, Tummon, F and Thouret, V 2014 Trajectory matching of ozonesondes and MOZAIC measurements in the UTLS – Part 2: Application to the global ozonesonde network. Atmos. Meas. Tech 7(1): 241–266. DOI: 10.5194/amt-7-241-2014
Stein, O, Schultz, MG, Bouarar, I, Clark, H, Huijnen, V, Gaudel, A, George, M and Clerbaux, C 2014 On the wintertime low bias of Northern Hemisphere carbon monoxide found in global model simulations. Atmos. Chem. Phys 14(17): 9295–9316. DOI: 10.5194/acp-14-9295-2014
Strode, SA, Worden, HM, Damon, M, Douglass, AR, Duncan, BN, Emmons, LK, Lamarque, J-F, Manyin, M, Oman, LD, Rodriguez, JM, Strahan, SE and Tilmes, S 2016 Interpreting space-based trends in carbon monoxide with multiple models. Atmos. Chem. Phys 16(11): 7285–7294. DOI: 10.5194/acp-16-7285-2016
Tanimoto, H, Zbinden, RM, Thouret, V and Nédélec, P 2015 Consistency of tropospheric ozone observations made by different platforms and techniques in the global databases. Tellus B 67. DOI: 10.3402/tellusb.v67.27073
Thouret, V, Marenco, A, Logan, JA, Nédélec, P and Grouhel, C 1998 Comparisons of ozone measurements from the MOZAIC airborne program and the ozone sounding network at eight locations. J. Geophys. Res , 103(D19): 25695–25720. DOI: 10.1029/98JD02243
Tilmes, S, Lamarque, J-F, Emmons, LK, Conley, A, Schultz, MG, Saunois, M, Thouret, V, Thompson, AM, Oltmans, SJ, Johnson, B and Tarasick, D 2012 Technical Note: Ozonesonde climatology between 1995 and 2011: Description, evaluation and applications. Atmos. Chem. Phys 12(16): 7475–7497. DOI: 10.5194/acp-12-7475-2012
Tressol, M, Ordonez, C, Zbinden, R, Brioude, J, Thouret, V, Mari, C, Nedelec, P, Cammas, J-P, Smit, H, Patz, H-W and Volz-Thomas, A 2008 Air pollution during the 2003 European heat wave as seen by MOZAIC airliners. Atmos. Chem. Phys 8(8): 2133–2150. DOI: 10.5194/acp-8-2133-2008
Worden, HM, Deeter, MN, Edwards, DP, Gille, JC, Drummond, JR and Nédélec, P 2010 Observations of near-surface carbon monoxide from space using MOPITT multispectral retrievals. J. Geophys. Res 115(D18): 314. DOI: 10.1029/2010JD014242
Worden, HM, Deeter, MN, Frankenberg, C, George, M, Nichitiu, F, Worden, J, Aben, I, Bowman, KW, Clerbaux, C, Coheur, PF, de Laat, ATJ, Detweiler, R, Drummond, JR, Edwards, DP, Gille, JC, Hurtmans, D, Luo, M, Martínez-Alonso, S, Massie, S, Pfister, G and Warner, JX 2013 Decadal record of satellite carbon monoxide observations. Atmos. Chem. Phys 13(2): 837–850. DOI: 10.5194/acp-13-837-2013
Yamasoe, MA, Sauvage, B, Thouret, V, Nédélec, P, Le Flochmoen, E and Barret, B 2015 Analysis of tropospheric ozone and carbon monoxide profiles over South America based on MOZAIC/IAGOS database and model simulations. Tellus B 67: 27884. DOI: 10.3402/tellusb.v67.27884
Yoon, J and Pozzer, A 2014 Model-simulated trend of surface carbon monoxide for the 2001–2010 decade. Atmos. Chem. Phys 14(19): 10465–10482. DOI: 10.5194/acp-14-10465-2014
Yu, KN, Cheung, YP, Cheung, T and Henry, RC 2004 Identifying the impact of large urban airports on local air quality by nonparametric regression. Atmos. Environ 38(27): 4501–4507. DOI: 10.1016/j.atmosenv.2004.05.034
Zbinden, RM, Thouret, V, Ricaud, P, Carminati, F, Cammas, J-P and Nédélec, P 2013 Climatology of pure tropospheric profiles and column contents of ozone and carbon monoxide using MOZAIC in the mid-northern latitudes (24°N to 50°N) from 1994 to 2009. Atmos. Chem. Phys 13(24): 12363–12388. DOI: 10.5194/acp-13-12363-2013