The IASI instrument has been developed to fly on board the MetOp polar-orbiting platforms. The first two platforms, MetOp-A and B, were successfully launched in 2006 and 2012 respectively. IASI is a nadir-viewing Fourier transform spectrometer observing the Earth–atmosphere thermal infrared radiation in the 645–2760 cm-1 wavenumber region (see, e.g., ) with a resolution of 0.5 cm-1 after apodization. IASI provides global Earth coverage twice a day, with an overpass time at ∼ 09:30 and ∼ 21:30 local time and a pixel size on the ground of 12 km at nadir.

IASI's primary objective is the delivery of accurate meteorological products to help to improve operational weather predictions. The IASI sensor can also monitor the tropospheric content of atmospheric trace gases such as O3 and CO . In the present study, we use data provided by the Software for a Fast Retrieval of IASI Data (SOFRID) presented in for O3 and in for CO. In their study, showed that IASI enabled the independent retrieval of O3 in the lower–middle troposphere (surface–225 hPa) and in the UTLS (225–70 hPa) in the tropics. Moreover, comparisons of SOFRID O3 data with data from O3 sondes have shown that the agreement is especially good for the UTLS column (225–70 hPa) with correlation coefficients of 0.8 (resp. 0.95) and biases of 17.5 ± 20 % (resp. 10 ± 10 %) in (resp. ). The ability of SOFRID to capture O3 daily variations in the tropical upper troposphere has also been demonstrated and validated against MOZAIC cruise data in . The SOFRID CO data have been validated against MOZAIC data in . SOFRID data are able to capture the seasonal variability of CO at midlatitudes (Frankfurt) as well as at tropical latitudes (Windhoek) in the lower (upper) troposphere with correlation coefficients of 0.85 (0.70). At Windhoek, in the lower (upper) troposphere SOFRID CO data are biased low with 13 ± 20 % (4 ± 12 %) compared to MOZAIC data.

The MOZAIC program was set up to provide routine measurements of reactive gases on long-distance commercial aircraft . In 1994, five airliners were equipped with O3 and relative humidity instruments, and a CO analyzer was successfully added in December 2001. MOZAIC aircraft operations have stopped at the end of 2014. However, since 2011, a new set of instruments has been flying on commercial in-service aircraft in the frame of the IAGOS (In-service Aircraft for a Global Observing System) Research Infrastructure. IAGOS builds on the scientific and technological experience gained within the two predecessors programs: MOZAIC and CARIBIC (http://www.caribic-atmospheric.com). The MOZAIC and IAGOS data follow the same calibration and quality control procedures and are freely accessible for scientific use at http://www.iagos.fr. The MOZAIC and IAGOS data are freely accessible for scientific use at http://www.iagos.org. These measurements are carried out with a 30 (4) s response time corresponding to a resolution of about 7 (1) km at cruise altitude and a vertical resolution of about 300 (30) m during ascents and descents, with a reported precision of ±5 (1) ppbv for CO (O3; ). For the present study, we used MOZAIC profiles measured at take off and landing near Hyderabad (17.2∘ N, 78.3∘ E) in central India from May to October 2009. CO data were available for each month but for O3 no data were produced in September and October following an instrument failure. For both gases, we could use from 10 to 16 profiles for each month with available data.

In order to compute the CO and O3 budgets in the Asian upper troposphere, we use the GC global chemistry transport model version 9-01-01 with a setup similar to that described in . This model has been thoroughly evaluated over the tropics through comparisons with in situ and remote sensed measurements of O3, CO, NO2 and HNO3 (e.g., ). GC is driven offline by the meteorological analyses from the Goddard Earth Observing System (GEOS-5) of the NASA Global Modeling and Assimilation Office (GMAO). Tropospheric chemistry includes both O3–NOx hydrocarbons and aerosols chemistry. Stratospheric O3 chemistry is computed with the linearized Linoz stratospheric ozone scheme developed by . STE are diagnosed with tagged O3 simulations including a stratospheric O3 tracer. Convection is parameterized with the relaxed Arakawa–Schubert scheme in GEOS-5. Turbulent mixing in the planetary boundary layer is described in . The simulations are performed on a regular 2∘ × 2.5∘ horizontal grid and on 47 hybrid sigma-pressure levels from the surface up to 0.01 hPa. Emissions from biomass burning (BB) come from the monthly Global Fire Emissions Database version 2 (GFED-v2) . The global anthropogenic emissions are taken from the EDGAR v.4.1 inventory, which provides annual global emissions of greenhouse gases and ozone precursors on a 1∘ × 1∘ horizontal grid, but typically the anthropogenic emissions are overwritten by data from various regional inventories. For instance over Asia we use the detailed inventory from . Regional emission inventories are also used over Europe (EMEP), Canada (CAC), Mexico (BRAVO) and North America (EPA/NEI99 with ICARTT modification). All anthropogenic inventories are scaled for the year 2005. Biogenic emissions are taken from MEGAN v2.1. Detailed information on these emission inventories can be found at http://acmg.seas.harvard.edu/geos/doc/archive/man.v9-01-01/index.html. NOx emissions from lightning are computed according to cloud top height parameterization , rescaled with LIS-OTD climatology () and are estimated at almost 6 Tg(N) year-1 .

We have performed 11 simulations for the May to October (MJJASO) period of 2009 with a 6-month spin-up. The control run was performed with all the emission sources considered. In order to determine the relative importance of the different sources on the CO and O3 Asian UTLS budgets, we have performed sensitivity runs with emissions alternatively switched off. For CO, the sensitivity simulations concern South (0–40∘ N, 60–100∘ E), East (15–40∘ N, 100–125∘ E) and Southeast 10∘ S–15∘ N, 100–150∘ E) Asian anthropogenic and African (20∘ S–20∘ N, 20∘ W–50∘ E) BB emissions. For O3, we considered the impact of NOx surface emissions from the same sources as for CO and the impact of LiNOx emissions from the two monsoon regions, South Asia (0–40∘ N, 60–100∘ E) and Africa (20∘ S–20∘ N, 20∘ W–50∘ E). In order to investigate the stratospheric contribution on the AMA tropospheric ozone budget (Sect. ), we use a tagged ozone tracer to follow the stratospheric ozone flux across the tropopause as used in and described by . The tagged simulation submits ozone produced in different regions of the atmosphere to archived three-dimensional fields of production and loss frequencies, allowing tropospheric ozone to be deconstructed into components from stratosphere and troposphere. The results from the sensitivity simulations are described and analyzed in Sect.  for the CO budget and in Sect.  for the O3 budget.

In order to validate the CO and O3 distributions simulated by the GC model, we use SOFRID CO and O3 retrievals to have a regional view of these distributions. The comparisons are made for monthly averaged profiles on the 2∘ × 2.5∘ GC grid. The GC profiles are first interpolated on the 43 vertical retrieval levels from SOFRID. IASI vertical profiles have a vertical resolution (∼ 6–8 km) that is much lower than those modeled by GC (100 m to 1 km). In order to take these resolution differences into account and make a sound comparison, we have to convolve the GC vertical interpolated profiles with IASI averaging kernels (AvK) according to the classical smoothing equation (e.g., ):

x^GC=xa+A⋅(xGC-xa), where xGC and x^GC are the original and the smoothed or convolved GC profiles. A is the SOFRID AvK matrix which describes the sensitivity of the retrieved to the true profile (see , for a description of the AvK matrix) and xa is the a priori profile used for the retrieval (the description of the a priori profiles can be found in for O3 and for CO).

The monthly distributions of UTLS (270–110 hPa) CO columns from IASI and GC are displayed in Fig.  for the region extending from Africa to Indonesia and from 10∘ S to 40∘ N for the May (pre-monsoon) to October (post-monsoon) period. The dominant features of these distributions are the maxima over Africa and Asia. The statistics of the CO UTLS columns comparison (for the domain displayed in Fig.  and the 6 months from May to October) are summarized in Table . GC underestimates the columns by 11 ± 9 % relative to IASI with a correlation coefficient of 0.70. The smoothing has little impact on the bias but reduces the relative standard deviations of the differences and enhances the correlations. The comparison between GC simulations forced with GEOS-5 analyses and MLS at 215 hPa for the tropical band of gives similar results with a 10 ppbv bias and a correlation coefficient of 0.65.

Over Africa the observed maximum shifts from western Africa in May to central and southern Africa in July and September following the BB season . We notice that the GC upper-tropospheric CO distributions over Africa display the same kind of discrepancies with IASI than those shown by with MLS. Indeed, their GC simulations have CO concentrations that are systematically too low at 215 hPa over central Africa in July and from August to October . Furthermore, have shown that five CTMs using GFEDv2 for BB emissions underestimate the upper-tropospheric CO concentrations during the monsoon over Africa between 10∘ S and 5∘ N by up to 50 ppbv compared to MOZAIC in situ data. The use of the BB emission inventory from leads to a correction of these biases and even to an overestimation of modeled upper-tropospheric CO over Africa. The bias documented here probably results from too low BB emissions over central and southern Africa from GFEDv2. Nevertheless, African BB emissions are not expected to impact the AMA composition and the observed biases will not impact our results.

Over Asia, which is the focus of our study, the highest CO columns are simulated by GC and detected by IASI over East Asia before the monsoon (May), over the continental convective region corresponding to northern India, Nepal and southern Tibet during the monsoon (JJA) and back over East Asia after the monsoon (September–October). We have used a threshold of 2.5 kg m-2 s-1 for the upward convective mass flux from the GEOS-5 analyses in the upper troposphere (350–150 hPa) to identify the deep convective areas (see contours in Fig. ). The ASM region is indeed characterized by GEOS-5 upward convective mass-flux values comprised between 1 and 5 kg m-2 s-1 in the upper troposphere (not shown) and 2.5 kg m-2 s-1 corresponds to relatively strong convective uplift. During July and August, high CO UTLS columns are also captured by the model and IASI within the AMA, as has already been documented in and . The AMA is delimited by the 12 520 m geopotential height (GH) contour at the 200 hPa level, as done in (see Sect.  for the definition of the AMA boundaries). More specifically, IASI detects enhanced CO columns in agreement with raw GC columns over the monsoon region and underestimates the CO columns in the western part of the AMA. This is an effect of IASI's limited vertical sensitivity, as appears from the GC UTLS distributions once the profiles are smoothed by IASI averaging kernels according to Eq. () (Fig.  second row) resulting in lower UTLS columns and a better agreement with IASI. This is confirmed by the longitude–pressure cross sections averaged over the 21–29∘ N band that correspond to the southern part of the AMA (Fig. ), where we notice that the AvK smoothing mixes the UTLS enhanced concentrations throughout the middle and upper troposphere, leading to a better agreement with IASI cross sections. In the eastern part of the AMA, CO UTLS concentrations are higher and better detected by IASI, resulting in a lesser effect of the smoothing and a better agreement between IASI and GC raw columns. Our results apparently disagree with , who report larger underestimations of UTLS GC CO over Asia than elsewhere in July 2005 especially at 100 hPa. They argue that this model underestimation probably results from insufficient convective uplift to 100 hPa with GEOS-5. Indeed, our comparisons with IASI (Fig. ) do not show enhanced underestimation of the GC UTLS columns in the Asian region and in the AMA. The low vertical resolution of IASI and its lack of sensitivity above 150 hPa highlighted in Fig.  are probably responsible for this apparent contradiction with .

The good agreement of IASI and GC in the middle and upper troposphere within the enhanced CO region is confirmed by looking at the latitude–pressure cross sections averaged over the 75–105∘ E longitude domain where convection is active (Fig. ). IASI clearly detects the UTLS enhanced CO concentrations between 400 and 200 hPa resulting from convective detrainment in very good agreement with GC. have already shown that the MOPITT sensor was able to detect UTLS CO enhancements disconnected from the lower troposphere and resulting from convective detrainment during the ASM. Our IASI latitude–pressure cross sections clearly show that IASI is also able to detect such CO UTLS bubbles. Both IASI and GC document that the southern edge of the CO enhancements shifts from 10 to 20∘ N from May to July and back to 10∘ N from August to October (Fig. ). Nevertheless, GC underestimates CO throughout the troposphere around 15∘ N particularly in May–June. These results are confirmed by CO profiles measured by the MOZAIC programme in Hyderabad (Fig. ). In the middle and upper troposphere, the agreement between MOZAIC and GC is within the 1σ variability, except during the May–June period, characterized by an important CO underestimation by GC, with nonetheless good modeling of the CO seasonal variation. Finally, enhanced UTLS CO columns from August to October over Indonesia also correspond with CO enhanced concentrations between 500 and 200 hPa at the Equator in both IASI and GC distributions in Fig. .

Even though the focus of our study is the upper troposphere, we note that, during the May–October period, high CO concentrations are detected by IASI and simulated by GC in the lower and middle troposphere within the monsoon polluted region over 20–35∘ N (Fig. ) and 70–120∘ E (Fig. ). Enhanced CO concentrations (> 110 ppbv) are also detected by IASI west of 70∘ E over the Middle East and northern Africa (Fig. ) where the model simulates lower CO concentrations even when the model–satellite bias is partly corrected when smoothing by the AvK is taken into account. The smoothing is responsible for mixing high CO concentrations simulated close to the surface to the lower and free troposphere. The discrepancy between GC and IASI in the free troposphere is larger between May and August than in September–October. The study of also documents an underestimation by GC of TES (Tropospheric Emission Spectrometer) for CO at 681 hPa over the Middle East and northern Africa that is larger in August than in September and October 2005 (see their Fig. 3). The underestimation of CO by the GC in the lower and middle troposphere also appears south of 20∘ N in Fig. . Comparisons between GC and MOZAIC profiles in Hyderabad (Fig. ) confirm these overly low CO concentrations simulated by GC below 600 hPa with decreasing differences from June to October.

Concerning the upper troposphere, both GC and IASI are able to capture the seasonal variability associated with the ASM and particularly the CO enhancements within the AMA. It is noteworthy that IASI enables the detection of uplifted CO in the ASM region. Nevertheless, GC significantly underestimates CO in the lower and middle troposphere during boreal spring over India compared with IASI and MOZAIC.

Concerning O3 GC vs. IASI comparisons, it is important to note that using Eq. () to smooth GC profiles implies mixing stratospheric O3 concentrations in the UTLS column. The averaging kernels displayed in show for instance that the O3 concentration retrieved at 150 hPa is sensitive to O3 up to about 50 hPa. Stratospheric biases in the model would therefore imply an apparent bias in the modeled UTLS column compared with IASI. As mentioned above, we use GC version 9-01-01, in which stratospheric O3 is based on the linearized scheme from . Recently have evaluated stratospheric O3 from GC version 9 (using Linoz) vs. a new version (not publicly available at the time of this study) using the Universal tropospheric–stratospheric Chemistry eXtension (UCX). They show that, averaged annually, GC-Linoz total columns of ozone are biased by 25 to 50 DU compared with TOMS in the band from 40∘ S to 40∘ N. The annual averaging hides much larger regional and seasonal discrepancies. Indeed, from their Fig. 2 we can roughly estimate that for the May–October period of interest here, the overestimation of the total columns can reach 100 DU in the tropics and in the Southern Hemisphere, down to 60∘ S. From , we also know that SOFRID stratospheric O3 is highly biased compared to ozonesondes with biases of 8 ± 5 % for the column up to 30 km and 7 ± 5 % for the stratospheric (16–30 km) column. Comparisons between IASI and GC for the May–October period in the 30∘ S–30∘ N band show that the mean GC stratospheric (90–24 hPa) column is 1.66 times higher than IASI mean column. Taking the 7 % IASI bias in the tropics into account, we have applied a 0.58 scaling factor to GC profiles in the lower and middle stratosphere (90–24 hPa) before applying the AvK smoothing.

The UTLS O3 columns are displayed in Fig. . The most obvious feature of the distributions captured by IASI and GC is the transition from low columns in the tropical UT south of the tropopause (2PVU) to high columns in the extratropical lower stratosphere. This transition closely follows the undulation of the tropopause. From June to September, the tropopause is pushed northwards by the AMA circulation and the region from the Middle East to East Asia is characterized by intermediate O3 columns. The region of lowest O3 columns is simulated and observed over the western Pacific in May and progresses northwestwards to Southeast Asia and South India until October. Over Africa, IASI and GC document a southward shift of moderate O3 columns from western Africa in May to southern Africa in September–October. This general good agreement between IASI and GC O3 distributions translates into correlation coefficients higher than 0.9 and a mean bias of 14 ± 26 % (see Table ). Biases between IASI-SOFRID and UTLS columns from ozonesondes were estimated to be 17.5 ± 19.3 % and 10 ± 10 % once the ozonesondes profiles were smoothed by IASI AvK. The mean value of the GC UTLS columns over our study region is therefore most likely to be in good agreement with ozonesondes. The good behavior of GC UTLS O3 is corroborated by comparisons between GC and MOZAIC profiles at Hyderabad which show a very good agreement between the surface and 200 hPa during the May–August period (see Fig. ). Unfortunately, no O3 data are available from MOZAIC Hyderabad–Frankfurt flights in September and October 2009.

When smoothing is applied to GC profiles, the features of the O3 distribution remain similar but some corrections are introduced. Over most of the domain, the GC UTLS columns are slightly increased, leading to a better agreement with IASI with differences within ±50 %. However, over the oceanic convective regions of the western Pacific characterized by the lowest O3 absolute values, the smoothing tends to decrease the UTLS column, leading to the highest relative biases (exceeding -50 %). This decrease of UTLS O3 when IASI AvK are applied has already been reported in for ozonesonde profiles as a result of the accentuation of the O3 S-shape for tropical profiles. The effect is therefore more important for convective oceanic profiles which have the most marked S-Shape.

The latitude–pressure cross sections displayed in Fig.  highlight the impact of the convolution of the modeled profiles by IASI AvK to smooth the lower stratosphere to upper troposphere transition and to decrease the height of the chemical tropopause. The very low O3 concentrations from the model-smoothed profiles over the Bay of Bengal convective region (south of 20∘ S) result from the accentuation of the S-shape profiles discussed above. These cross sections also indicate the northwards shift of the tropopause and of high UTLS (300–150 hPa) O3 concentrations from May until September. It is interesting to note the large O3 concentrations originating from the stratosphere in the middle troposphere down to 700 hPa between 20 and 30∘ N in May and June that almost disappear in July and August, only to reappear in October. The seasonal variations of STE that both model and observations are pointing to are in good agreement with the results from which, based on in situ data in the Himalaya, indicate the absence of stratospheric intrusions during the monsoon season.

Figure presents the O3 longitude–pressure transects over Asia. In the middle–upper troposphere, both model and observations display a persistent west–east gradient with lower O3 concentrations east of 70∘ E. This gradient is the highest during the Asian monsoon period when convection is the most active in the western part of the domain and when the Middle East is characterized by its annual O3 maximum (). Nevertheless, from June to September, the UT O3 concentrations are not homogeneously low in the convective region and enhanced O3 concentrations are simulated and observed between 100 and 120∘ E. In the model, the lowest UT O3 concentrations coincide with the deepest convection centered around 75∘ E, and the enhanced concentrations coincide with less intense convection, as illustrated by the 2.5 kg m-2 s-1 convective upward mass-flux contour.

The general features of the tropospheric and UTLS O3 distribution over the large Asian region simulated by the GC are in good agreement with those observed by IASI. The application of the AvK convolution to GC vertical profiles decreases the altitude of the chemical tropopause, smoothes some of the modeled high-resolution features and accentuates the S-shape of convective oceanic O3 profiles. Nevertheless, the model and IASI display the same longitudinal and latitudinal gradients, both in the middle and in the upper troposphere over Asia.

During May and October, the convective activity mostly takes place over Southeast Asia and the 150 hPa tropopause is located between 30 and 35∘ N over Asia and the AMA is not present (see Fig. ). In June and September, at the beginning and at the end of the ASM, the convective activity has moved northwards towards the Bay of Bengal and the AMA is present over northeastern South Asia. During the heart of the ASM (July–August), the region impacted by convection encompasses the Bay of Bengal, India, Bangladesh, Nepal and southeastern Tibet and the tropopause is pushed to 40∘ north by the AMA, which is fully developed and extends roughly from 20 to 40∘ N and from 30 to 120∘ E and vertically from 300 to 100 hPa. The center of the AMA is bimodal with the high-pressure center located alternatively over the Tibetan plateau and over Iran . This high-level anticyclone is characterized by large-scale periodic elongations and shedding as described in . The AMA air masses are characterized by low potential vorticity (PV) values or high GHs. Based on MLS CO analyses, have shown that daily CO and PV variations were strongly correlated with low PV related to high CO. In the Asian UTLS, the tracer concentration is therefore strongly controlled by the oscillations and shedding of the AMA. In their study of the AMA strength and variability, also pointed to the spatiotemporal correlation of CO enhancements and low PV values which is stronger in the upper levels of the AMA. Based on PV fields have developed a method to characterize the dynamical barrier that delimit the inside and the outside of the AMA on a daily timescale. The boundaries of the AMA based on their method are consistent with tracer concentrations (high CO and low O3 within the AMA). In studies looking at monthly or seasonal timescales, the edge of the AMA has been mostly defined as simple constant GH contours at different pressure levels. () use a 14 320 (14 430) m GH for the AMA at 150 hPa and use 12 520 (16 770) m GH at 200 (100) hPa.

In order to determine the CO and O3 budget within the AMA, we first need to characterize the AMA as a closed volume and we have therefore looked for a criterion independent of the pressure level. As already discussed, the studies based on PV have shown that it was a good dynamical parameter to characterize the AMA high-frequency variability whilst GH was mostly used on monthly timescales . Furthermore, is the only study that proposes a PV-based criterion to delimit the AMA but this criterion is only defined and validated for the 380 K potential temperature level (∼ 200 hPa). As the PV tracer relationship is stronger at the higher levels (380 K) of the AMA the criterion from may not hold for the lower levels. Finally, on monthly timescales, simple GH thresholds have been shown to consistently delimit regions of tracer anomalies characteristic of the AMA at different pressure levels. We have therefore chosen to use a criterion based on GH rather than PV to delimit the AMA. Our criterion is based on thresholds of GH anomalies. We use the GH monthly fields from the MERRA re-analyses, which are provided on 42 levels from the surface to 0.1 hPa with a 1.25∘ × 1.25∘ horizontal resolution. The anomalies are computed as the differences between the mean zonal GH computed over the 50∘ N to 50∘S latitudinal band and the local GH. The AMA appears very clearly at different UTLS levels as the region with the highest GH anomalies on Fig. . The contours corresponding to a 270 m GH anomaly best match the 16 770, 14 320 and 12 520 m GH isocontours at 100, 150 and 200 hPa corresponding to the AMA edge in , and , respectively. We have therefore chosen a 270 m GH anomaly as the threshold for the AMA boundary throughout the UTLS. In Sect. , within the AMA and outside of the AMA both refer to the tropospheric part of these atmospheric regions bounded by the 2PVU contour.

The studies presented in the introduction have highlighted the AMA as a region with a composition that is very different from its surroundings, according to UTLS satellite observations. The use of IASI data brings information about CO and O3 over the whole troposphere and therefore allows us to better document the link between the upper-tropospheric distributions and transport processes such as convection. In the following paragraph, we analyze the modeled and observed O3 and CO distributions in light of their relationship with convection.

In the middle troposphere, the longitude–pressure sections of CO and O3 presented above are anti-correlated. East of about 80∘ E, in the monsoon region characterized by the strongest convective upward mass fluxes from GEOS-5, high CO (90 ppbv) is associated with low O3 (60 ppbv) and west of 80∘ E low CO is associated with high O3. This anti-correlation is clear both from the model outputs and from IASI data. The high summer tropospheric O3 extending from western India to northern Africa has been first described as the“Middle East tropospheric ozone maximum” by and further analyzed by . The subsidence associated with the AMA is taking place in the middle troposphere on its western side over the Eastern Mediterranean, the Middle East and Central Asia . This phenomenon is clearly seen in Fig. , which displays GC O3 fluxes in a longitude–pressure cross section at the center of the AMA. This descent of air masses impacted by Asian pollution trapped within the AMA contributes to the summer “Middle East tropospheric ozone maximum”. In their analysis, have shown that the O3 buildup is favored by the Arabian and Saharan anticyclones that isolate the middle troposphere over this region. From simulations with tagged O3, attribute an equivalent and dominant impact (30–35 %) on the O3 maximum over the Middle East to local sources and transport from Asia via the UT and the AMA circulation. Over northern Africa, transport from Asia contributes less than regional sources. It is clear from the CO GC distributions displayed by (their Fig. 6) and from the present study as well as from our IASI data (Figs.  and ) that the O3 Middle East maximum in the middle troposphere coincides with relatively low CO concentrations.

Between 80 and 120∘ E, the low O3 and high CO concentrations result from the convective activity occurring in South and Southeast Asia during the monsoon. Convection mixes CO between the Asian polluted PBL and the upper troposphere, resulting in enhanced concentrations over the whole troposphere. The overlap between important CO sources and convection occurs primarily over the Indo-Gangetic Plain (IGP) according to Fig. , which displays anthropogenic CO emissions from the Streets inventory and GEOS-5 upward convective mass fluxes. The impact of convective transport on the O3 distribution is more complicated. It results from two antagonist effects: the vertical mixing of O3 itself and the uplift of O3 precursors followed by enhanced photochemical O3 production . The vertical mixing results in the transport of O3-poor air masses from the lower troposphere, where O3 lifetime is short, to the upper troposphere, where it is long, and the transport of O3-rich air masses from the upper to the lower troposphere by compensatory subsidence. The effect of this overturning is a decrease of UT O3 and of the tropospheric O3 burden and lifetime. Over polluted regions, such as Asia, convection uplifts O3 precursors (especially NOx) result in an increase of the O3 production in the middle and upper troposphere at the expense of the lower troposphere. The electric activity from convective storms is responsible for the in situ production of LiNOx, also responsible for an increased O3 production. This source of O3 clearly appears in Fig.  where the net O3 production rates are enhanced between 500 and 150 hPa in the monsoon region. Convective clouds also diminish the tropospheric photochemical activity through a reduction of the solar UV radiations. These combined effects are responsible for the lower mid-tropospheric O3 concentrations over South Asia compared to regions with high insolation and downward transport of O3, such as the Middle East and northern Africa.

In the Asian upper troposphere in June, the AMA builds up and only extends between 60 and 120∘ E and the O3 fluxes switch from downward to upward around 90∘ E (Fig. ). In July and August, the AMA is well established over the 15–145∘ E domain and the upward flux remains east of 90∘ E in the monsoon region while the strongest downward fluxes move to the western edge of the AMA between 15 and 45∘ E. As already discussed, this downward flux partly contributes to the buildup of the Middle East O3 maximum as described in . In September, the situation is similar to June: the AMA has largely shrunk and the O3 production is associated with an O3 downward flux between 75 and 90∘ E. Above the continents, the photochemistry illustrated by the O3 net production rates in Fig.  switches from a net source of O3 in the polluted PBL to a net sink in the free troposphere below about 500 hPa and again to a net production in the middle and upper troposphere. This behavior agrees with the different NOx photochemical regimes discussed in . In particular, low NOx concentrations are responsible for the destruction of O3 in the lower and middle troposphere and slightly higher concentrations produce O3 in the upper troposphere, as explained in Brune (1992; IGAC Report). During the whole period, the O3 net production pattern in the middle and upper troposphere is characterized by a double maximum with values exceeding 5 ppbv day-1, which are associated with the upward fluxes east of 90∘ E and downward fluxes (except in August) west of 90∘ E. Both upper troposphere maxima are located within the eastern half of the AMA. Below the tropopause, the O3 net production rate exceeds 2 ppbv day-1 within the whole AMA. The enhanced net O3 production rates are associated with enhanced NOx concentrations (100 pptv contour in white). In the upper troposphere, the AMA therefore appears as a region of high O3 production, resulting from the trapping of NOx from various sources. In the next section, we determine the impact of the different sources on the CO and O3 budgets within the AMA.

As mentioned in Sect. , we have considered the two main regions of importance concerning anthropogenic CO emissions: South and East Asia. and have indeed highlighted the predominant role of Asian sources from these two regions in filling the AMA with CO. We can also notice that the surface fluxes of CO used for our GC simulations (Fig. ) are the largest for the whole Asian region over northeastern China and for the South Asian domain over the IGP. These fluxes are consistent with those used in and . Concerning BB, have shown that Indonesian BB emissions had a large impact on the Indian upper-tropospheric composition in 2006 following the perturbation of the tropical circulation by a strong El Niño event. Our sensitivity simulations performed for Indonesian or Southeast Asian anthropogenic sources have shown that in 2009 this region did not impact the South Asian upper troposphere (not shown). The simulation with African BB CO emissions switched off also results in negligible modifications of the CO distribution in the South Asian upper troposphere (not shown).

The differences between the reference simulation and the sensitivity simulations with anthropogenic CO emissions from South and East Asia shut down are displayed in Fig.  for the pressure–longitude section (21–29∘ N) and in Fig.  for the upper-tropospheric (200 hPa) distribution. The average CO mixing ratio differences between on and off simulations within and outside of the AMA are given in Table . The pressure–longitude sections clearly show that the upper troposphere and especially the AMA ones are more impacted by South Asian than East Asian emissions. For the 4 months considered, CO from South Asia is responsible for CO enhancements of 20 to 30 ppbv within the AMA between 300 and 100 hPa, while East Asian emissions mostly impact regions below 200 hPa on the eastern side of the AMA. This result is expected from the correlation between high emissions and strong convection over South Asia as can be seen in Fig. . High convective mass fluxes (> 2.5 kg m-2 s-1) at 225 hPa are located over the IGP, where CO emission fluxes exceed 150 kg km-2 day-1. East of the Himalaya, the emissions are largest over eastern China where convection is not as strong as over the IGP. The region with the strongest South Asian CO uplift in the middle troposphere lies between 75 and 105∘ E according to the GC (see Fig. ), which is consistent with , who highlights that PBL air masses that reach the UTLS pass through a mid-tropospheric conduit located roughly over the same region.

In the upper troposphere at 200 hPa, East Asian emissions are only responsible for CO enhancements of about 10–20 ppbv located over Southeast Asia and China during the monsoon. Larger CO enhancements are caused by South Asian emissions with the highest values (> 35 ppbv) located within the convective region around 75∘ E and 27∘ N and values exceeding 20 ppbv that spread within the AMA bounded by the tropopause to the north. These values are higher than those of , who found CO enhancements of 12–30 ppbv from Indian sources and of 5–9 ppbv from Chinese sources at 215 hPa. At 100 hPa (not shown), East Asian sources contribute to less than 6 ppbv to UTLS CO, which is slightly lower than what and have documented. Concerning South Asian sources, they are responsible for 12 to 20 ppbv CO enhancements (not shown) in good agreement with and . have also quantified the origin of PBL air masses in the AMA using artificial emission tracers from the CLaMS CTM. Their emission regions are different from those used in the present study. India is separated into northern and South India and Southeast Asia encompasses our Southeast Asia and part of our East Asia (most of the Indochinese peninsula). Nevertheless, their results show some agreement with ours and give some complementary information. They show that when the AMA is established, PBL air masses coming from northern India fill up the AMA comparably to our South Asian tracer, which indicates that South India plays a minor role. Their Southeast Asian emission tracer is transported upwards and remains at the edge of the AMA such as our East Asian tracer (especially for August, which is not shown). The agreement probably comes from the fact that both tracers encompasses the Indochinese peninsula where convection is strong during the monsoon but which is located to the south of the AMA.

The average figures of Table  summarize these results. South Asian CO emissions are responsible for a strong CO enhancement within the AMA from June to September with a maximum of ∼ 25 ppbv during the monsoon peak in July–August. Furthermore, average CO enhancements from South Asian emissions are about 10 ppbv larger within than outside of the AMA, which further highlights the AMA as a trap for uplifted South Asian pollution during the monsoon. East Asian emissions result in maximum enhancements of about 10 ppbv in the UTLS during July–August. The little differences between the enhancements computed within and outside of the AMA also show that East Asian sources are located outside of the conduit connecting boundary layer air masses and the AMA described in .

The contribution to the O3 burden from the main sources of NOx emissions is computed from sensitivity simulations with the GC model. have shown that tropospheric O3 over Asia during the monsoon is mostly impacted by Asian sources. Focusing on the Indian region, have also highlighted the predominance of Asian sources (India, China and Indonesia) on the Indian tropospheric O3 budget during the monsoon. They have also shown that Middle East emissions have a small impact on NOx and O3 concentrations below 500 hPa and that African and Middle East sources have a negligible impact in the middle and upper troposphere over India during the ASM. We have therefore chosen to focus on the impact of Asian emissions upon the AMA O3 burden. Concerning anthropogenic emissions, we have separated Asia into the same three main regions as for CO (see Sect. ). One of the main conclusions of is that LiNOx is the most important NOx source controlling the tropical tropospheric O3 burden. We therefore performed simulations to characterize the importance of LiNOx from the two nearby monsoon regions (see Sect. ) upon upper-tropospheric O3 during the ASM. Finally, the impact of STE was established using the GC stratospheric O3 tagged tracer as explained in Sect. .

For O3, the results of the sensitivity simulations are displayed in Fig.  for longitude–pressure sections averaged over the 21–29∘ N band and in Fig.  for maps at 200 hPa. The results are summarized in Table  for O3 and NOx average mixing ratios. The enhancements of O3 by NOx anthropogenic emissions from South and East Asia are closely linked to those of CO previously analyzed. As for CO, sensitivity simulations with Indonesian anthropogenic and African BB NOx sources switched off (not shown) show very little impact on South Asian upper-tropospheric O3.

The O3 enhancements caused by East Asian emissions is the largest (> 15 ppbv) below 300 hPa between 90 and 120∘ E. Convection is not strong enough over China to bring PBL NOx deep into the AMA and, on average, upper-tropospheric O3 enhancements from Chinese emissions are about 5 ppbv both within and outside of the AMA during July–August. Compared to Chinese emissions, South Asian emissions have a smaller impact on free-tropospheric O3 (< 12 ppbv) but a larger-scale impact on O3 in the upper troposphere and more specifically within the AMA. On average, South Asian emissions are responsible for an O3 (resp. NOx) increase of 8 (resp. 0.04) ppbv within the AMA and of about 5 (resp. 0.015) ppbv outside of the upper-level anticyclone (Table ). Indian NOx is uplifted and trapped within the AMA (see white contours in Fig. ) and produces O3 molecules that are also trapped within the AMA.

Asian LiNOx is responsible for an important O3 production in the Asian upper troposphere mostly confined within the AMA (see Fig. h and i) with a strong intra-seasonal variability. In July, LiNOx produces 13.5 ppbv O3 in the AMA and only 10 ppbv in August. In both cases, the O3 production outside of the AMA is half of its value within the AMA. For NOx, the production within the AMA is about 2.5 higher than outside of the AMA, highlighting the nonlinearity of the O3 production by NOx. The impact of African LiNOx over Asia varies strongly from June to September. In June and September, when the AMA is weakened and located east of 90∘ E, African LiNOx has a large impact in the upper troposphere over the Middle East and in the free troposphere further east over India (Fig. ). In July and August, the AMA circulation that extends to 30∘ W prevents air masses impacted by African LiNOx from affecting O3 in the Middle East upper troposphere and the free troposphere over India is also less impacted than in June and September. During the July–August period, the large subsidence over the Middle East (30–60∘ E) (see Fig. b and c) brings O3 produced by both South Asian anthropogenic NOx and Asian LiNOx down to 400 hPa (Fig. e and h) and contributes to the upper part of the mid-tropospheric O3 maximum. Below 400 hPa and down to 600 hPa, the air masses coming from the west are not blocked by the AMA and both African LiNOx and STE have a larger contribution to the free-tropospheric Middle East O3 maximum (Fig. k and n) highlighted by GC and IASI (Fig. d and f) than Asian sources.

The last source of O3 in the Asian upper troposphere that we investigated are STE. At 200 hPa, STE are not an important contributor to the O3 distribution, as can be seen in Fig. . At this pressure level, stratospheric O3-rich air masses are kept outside of the AMA circulation. Nevertheless, on average, STE contribute from 7 to 12 ppbv O3 within the AMA (Table ). These high values are caused by STE impacting the upper troposphere between 150 hPa and the tropopause, as highlighted by the stratospheric O3 tracer cross sections in Fig. . It is also interesting to note that STE also impact the free troposphere over the Middle East and India in a very similar way to African LiNOx, traveling with the westerly winds below the AMA. The same eastward transport of Middle East NOx emissions has been shown to slightly (∼ 10 %) impact NOx and O3 distributions in the lower troposphere over India . Nevertheless, as discussed in Sect. , O3 from GC is overestimated in the lower and middle stratosphere (24–90 hPa) by a factor of ∼ 1.7. This overestimation most likely implies a similar overestimation in STE evaluated with the O3 stratospheric tracer and STE are probably responsible for a 4 to 7 ppbv O3 enhancement in the AMA.

Asian LiNOx therefore appears to be the largest NOx source within the AMA with a contribution to the NOx concentration that is 2 to 3 times larger than South Asian anthropogenic NOx emissions. This result appears contradictory to that of , who estimated that during the monsoon in the Indian upper troposphere 60 to 70 % of NOx come from local surface sources and only 20–25 % from LiNOx. This apparent contradiction is due to the fact that define the upper troposphere as the 500–150 hPa while the AMA spans the 300–100 hPa domain and, according to Fig. , LiNOx has its largest impact between 200 and 100 hPa. Furthermore, the global annual LiNOx source used in is 2.8 Tg(N) year-1, which is in the lower part of the 6 ± 3 Tg(N) year-1 estimation from . In our GC simulations, the global annual LiNOx source is set to 6 Tg(N) year-1. Concerning the impact of NOx local sources on the upper-tropospheric (500–150 hPa) O3, found a maximum of 15 %. Similar results are found by with a 10 to 20 % sensitivity of O3 to Indian NOx emissions in the middle and upper troposphere (700–200 hPa) over India. From Fig. e and f, we can roughly estimate a production of 9 ppbv in the 500–150 hPa range and 60–95∘ E by Indian NOx sources. For the same region, we also estimate a rough average of 60 ppbv O3 for the July–August period from Fig. g and j. We have therefore an approximate 15 % sensitivity of O3 to the Indian NOx source in good agreement with . According to , NOx emissions from Indonesia have a non-negligible effect on upper-tropospheric NOx (20–30 %) and O3 (10–15 %) over India during the ASM period. They also state that the impact of Indonesian emissions is more important over the southern part of India through transport by the tropical easterly jet, which was especially strong in the 1997 El Niño year. This does not contradict the negligible impact of Indonesian emissions on the AMA composition that we have reported, the AMA being an isolated region north of the tropical easterly jet.