Dynamics and composition of the Asian summer monsoon anticyclone

. This study places HALO research aircraft observations in the upper-tropospheric Asian summer monsoon anticyclone (ASMA) into the context of regional, intra-annual variability by hindcasts with the ECHAM/MESSy Atmospheric Chemistry (EMAC) model. The observations were obtained during the Earth System Model Validation (ESM-Val) campaign in September 2012. Observed and simulated tracer–tracer relations reﬂect photochemical O 3 production as well as in-mixing from the lower troposphere and the tropopause layer. The simulations demonstrate that tropospheric trace gas proﬁles in the monsoon season are distinct from those in the rest of the year, and the measurements reﬂect


Introduction
The Asian monsoon system is one of the largest and most dominant atmospheric features on Earth. It is stronger than other monsoon systems because of the topography of the region, which insulates warm, moist air over South Asia (the sub-Himalayan countries of the Indian subcontinent) from the cold and dry extratropics (Boos and Kuang, 2010). This leads to a global maximum of surface moist static energy at the south-western flank of the Himalayas (Boos and Hurley, 2013), which drives deep convective updraughts during Northern Hemispheric summer. Elevated surface heating over the Tibetan plateau (Flohn, 1960;Fu et al., 2006), predominantly northward surface winds plus orographic uplifting at the southern/south-western slopes of the Himalayas (Li et al., 2005;Y. Liu et al., 2009) and deep convection over the Bay of Bengal (Park et al., 2009;Nützel et al., 2016) all additionally contribute to an overall ascending air current. This drives an anticyclonic circulation, centred at 200 to 100 hPa (Dunkerton, 1995;Randel and Park, 2006;Garny and Randel, 2016).
The location, shape and strength of the Asian summer monsoon anticyclone (ASMA) strongly vary on intraseasonal, interannual and longer timescales (Dunkerton, 1995;Lin et al., 2008;Kunze et al., 2010;Pokhrel et al., 2012), which is subject to ongoing discussion Nützel et al., 2016). An elliptical vortex is intrinsically unstable (Hsu and Plumb, 2001;Popovic and Plumb, 2001), thus prone to splitting up and eddy shedding to the west and east (Dethof et al., 1999;Vogel et al., 2014). Vari-Published by Copernicus Publications on behalf of the European Geosciences Union.
able forcing by convection (Randel and Park, 2006;Garny and Randel, 2013), subseasonal oscillations (Lin et al., 2008;Goswami, 2012), the interaction with Rossby waves or midlatitude synoptic disturbances (Dethof et al., 1999) add further complexity. The overall upwelling in the eastern ASM region is accompanied by large-scale subsidence in the western part (Rodwell and Hoskins, 1996), making the Arabian Peninsula one of the warmest and driest regions on Earth. The heat low associated with the hot desert conditions in summer produces an anticyclone (Lelieveld et al., 2009) in the middle to upper troposphere, which interacts with the ASMA.
The interplay of the above dynamical ingredients makes the Asian summer monsoon a switch yard and mixing vessel for air masses of different origins and with different compositions, including the exchange between the troposphere and stratosphere. Monsoon air is received by regions around the globe  and was, for instance, shown to affect the tropospheric chemical composition in the Mediterranean (Lelieveld et al., 2001Scheeren et al., 2003). A mid-tropospheric (400-500 hPa) summertime O 3 maximum over the eastern Mediterranean/Middle Eastern region (Li et al., 2001;Lelieveld et al., 2009;Schuck et al., 2010;Akritidis et al., 2016) is enhanced by the Asian monsoon outflow (Y. Richards et al., 2013;Barret et al., 2016), but it is not clear whether O 3 in the ASMA plume is generally enhanced or depleted (Lawrence and Lelieveld, 2010).
In the following TL refers to the mixing zone at the tropopause, where cross-tropopause exchange of air masses on average creates a gradient between stratospheric and tropospheric trace gas signatures. The TL is also denoted by ExTL in the extratropics and TTL in the tropics, reflecting the changes in dominating physical processes at about the 30 • in latitude. There are no rigid boundaries, but rather stratospheric influence decreases towards the troposphere over a range of several kilometres (Gettelman et al., 2011). In contrast, "upper troposphere" (UT) is used here to describe the altitude region that is dominated by the ASMA. Despite its importance for redistributing trace gases between the boundary layer, troposphere and lower stratosphere, the highly variable composition of the ASMA and the processes behind it are not well understood yet .
In situ measurements were conducted in the ASMA during the Earth System Model Validation (ESMVal) field experiment with the High Altitude and LOng Range (HALO) research aircraft in September 2012. A sudden enhancement of measured O 3 when HALO entered the ASMA from the south was the motivation for the accompanying paper (Gottschaldt et al., 2017), since those measurements contrast with the presumption of decreased O 3 in the ASMA. It was shown that the ASMA filament(s) encountered during that flight were associated with entrainments of lower-/mid-tropospheric air at the eastern ASMA flank as well as with stratospherically influenced TL air.
Here we put the specific situation observed during the HALO ESMVal campaign into a regional, seasonal and multi-annual perspective, which is provided by global chemistry climate simulations with the ECHAM/MESSy Atmospheric Chemistry (EMAC) model.
Recent papers discussed climatological trace gas distributions in the monsoon region (Santee et al., 2017), CO distributions in the context of daily ASMA dynamics  and monthly budgets of CO and O 3 . Building on the ASMA observations during the HALO ESMVal campaign, the second objective of our study is to complement these papers by considering additional tracers on a 10-hourly scale to characterise key processes relevant for the O 3 distribution in the monsoon region.
We first briefly summarise the data used here, then discuss the EMAC-simulated intra-annual variability of selected tracers in the ASMA region for the year of the HALO ESM-Val campaign, put observed tracer-tracer relations in the context of simulated ones, discuss the interplay of the processes that contributed to the observed trace gas signatures and also show in the context of multiple monsoon seasons that the specific situation observed during the HALO ESMVal campaign was not exceptional. For brevity the main text only provides summarising statements about lightning NO x (LiNO x ) and reactive nitrogen (NO y ) in the ASMA, and we refer to the Supplement for details. Additional figures in the Supplement are provided for documentation and reproducibility.

Data
We focus on the analyses of O 3 , CO, hydrogen chloride (HCl) and reactive nitrogen (NO, NO x , NO y ), as those tracers reflect the processes most relevant for the interpretation of in situ measurements in the ASMA during the ES-MVal flight from Male (Maldives) to Larnaca (Cyprus) on 18 September 2012. All in situ measurements used here are based on a data set with a 10 s time resolution, which is available from the HALO database (https://halo-db.pa.op.dlr.de). The corresponding measurement techniques are described in the accompanying paper and in more detail in publications about the individual instruments: CO (Hoor et al., 2004;Schiller et al., 2008;Müller et al., 2016), HCl Voigt et al., 2014), NO/NO y (Ziereis et al., 2000) and O 3 . Among those tracers, only HCl mixing ratios were at the instrument's detection limit during the considered flight .
The transport pathways of air parcels before being encountered by HALO were calculated with the Lagrangian HYS-PLIT model (Draxler and Hess, 1998;Draxler and Rolph, 2015). Although published in the accompanying paper, those analyses are a basis for this study. In the following all simulation data stem from global chemistry climate simulations with the EMAC model (Jöckel et al., 2010), performed within the ESCiMo (Earth System Chemistry integrated Modelling) project (Jöckel et al., 2016) and the DLR-internal ESMVal project. Our reference simulation has been described and generally evaluated as RC1SDbase-10a by Jöckel et al. (2016). Its set-up is designed for the best possible comparability to observations by nudging the dynamics to ECMWF ERA-Interim (Dee et al., 2011) reanalysis data and covers the period 1980-2013 (excluding spin-up). Convection is not resolved in the simulation, but its effects are captured by a parameterisation in EMAC. LiNO x emissions are parameterised on top of the convection parameterisation. Given the above uncertainties, simulated lightning activity compares acceptably with satellite observations (Supplement). NO x background mixing ratios are crucial for O 3 photochemistry, as will be discussed in more detail in Sect. 6.3. In situ measurements are the most accurate in the UT. We have shown in the accompanying paper that this simulation reproduces the measured trace gas mixing ratios along the HALO flight track of 18 September 2012 reasonably well, but this comparison is rather limited, spatially and temporally. Therefore we compare simulated NO and NO y to one of the most comprehensive observational data sets available for reactive nitrogen in the UT : IAGOS-CARIBIC (In-service Aircraft for a Global Observing System -Civil Aircraft for the Regular Investigation of the atmosphere Based on an Instrument Container; Brenninkmeijer et al., 2007, http://www.caribic-atmospheric.com). Our comparisons are based on the output of the EMAC S4D submodel (Jöckel et al., 2010), which provides simulation data along the given IAGOS-CARIBIC flight tracks at each model time step ( t = 12 min). The agreement between simulated NO and corresponding IAGOS-CARIBIC observations is remarkable, particularly in the ASMA region (Supplement). Further comparisons between the EMAC RC1SD-base-10a simulation and IAGOS-CARIBIC are shown by Jöckel et al. (2016) for O 3 , CO and others, based on 10-hourly simulation output.
Ten-year averages of simulated O 3 reproduce the low-O 3 ASMA interior of satellite climatologies (Santee et al., 2017) as well as increased O 3 found by HALO ESMVal at slightly lower potential temperatures (Fig. 1).
Additional EMAC simulations were performed in quasichemistry transport model mode Gottschaldt et al., 2013) to test the impact of LiNO x . These are described in the Supplement. "Simulation" without further specification refers to RC1SD-base-10a in the following.

The ASMA region
As noted in the introduction, the ASMA is driven by a largescale updraught originating from the south-western flank of the Himalayas, on the one hand, and by smaller-scale tropical deep convection events, on the other hand. The latter correlates with a maximum of outgoing long-wave radiation (OLR), which expands from the Bay of Bengal towards the Tibetan plateau and back in the course of the monsoon season . In contrast, the large-scale updraught is tied to geographical features (maximum of moist static energy in the Indo-Gangetic plain, heating of the Tibetan plateau, orographic forcing of the Himalayas). The inland thermodynamic conditions of the Arabian Peninsula support the mid-tropospheric anticyclone in the west. It may intermittently merge with the ASMA, but we presume that the  Figure 2. CO mixing ratios and geopotential height (GPH) simulated by EMAC for the monsoon months of 2012. Enhanced CO is considered to be a chemical characteristic of the ASMA, and increased GPH is a dynamical proxy used to delimit the ASMA. The Iranian and Tibetan domains are used throughout the paper to discuss differences between the convectively driven eastern part and the western part that is mainly controlled by UT transport. The Iranian region was traversed by the HALO ESMVal campaign during a flight from Male (Maldives) to Larnaca (Cyprus) on 18 September 2012. Beads show the HALO positions at full UTC hours, and the chosen isentropic (a) or pressure (b) levels roughly correspond to UT flight sections. composition of the UT in the west is determined mainly by air transported in the eastern-driven circulation. We refer to the western and eastern parts as "Iranian" and "Tibetan", respectively. ASMA unspecifically refers to the whole system.
The regions' delimitations ( Fig. 2) for separate analyses of the different parts were chosen visually, considering the following: (i) to put the measurements into perspective, the regions shall capture the synoptic situation during the HALO ESMVal campaign; (ii) both parts shall be equally sized; (iii) the variability of the ASMA's location and extent shall be covered. The chosen meridional range of 15 to 35 • N covers the simulated ASMA ridgeline for most of the monsoon season (shown in Fig. 3b). The zonal ranges are 30 to 65 and 65 to 100 • E for the Iranian and Tibetan regions, respectively. For comparison, Yan et al. (2011) classified anticyclonic centres between 50 and 67.5 • E in Iranian mode, and between 80 and 92.5 • E in Tibetan mode.
We decided not to adapt the regions dynamically to the actual ASMA, because the boundary definitions we are aware of (Ploeger et al., 2015; Barret et al., 2016; emphasise the concept of a closed ASMA volume or transport barriers on monthly or seasonal timescales. However, the ASMA boundaries are not always well defined, particularly during transitions between different dynamical modes. Our pre-fixed regions allow an unbiased view on the effects of complex, 10-hourly dynamics. This comes at the price that features from outside the ASMA might contribute to the analyses occasionally. We cannot rule out that concurrent but geographically distinct features feign correlations between different species, but monsoon-related features should mostly dominate the lateral averages in the chosen regions. Our approach detects differences between Iranian and Tibetan parts, because the corresponding circulation is tied to the geographical features of these regions. Enhanced CO is considered to be a chemical characteristic of the ASMA , and increased geopotential height (GPH) is a dynamical proxy . Simulated seasonal mean distributions of both proxies indicate that our regions capture the ASMA of 2012 well (Fig. 2).
Large-scale transport occurs mainly on isentropes, unlike convective transport. Pressure and isentropic vertical coordinates are similar in the UTLS in the tropics of the Tibetan region (Fig. 4a). In the EMAC simulation the TP has been diagnosed by a potential vorticity of 3.5 PVU in the extratropics and by the WMO definition between 30 • N and 30 • S (Jöckel et al., 2006). It is almost parallel to one isentrope in the tropics and to a lower one in the extratropics, but intersects isentropes around 360 K almost perpendicularly in the transition region at about 30 • N. This facilitates isentropic in-mixing from the lower stratosphere or the TL, but only in combination with southward wind components. If winds follow the TP (e.g. subtropical jet), it is still a transport barrier. The latter aspect is relevant for stratosphere-to-troposphere trace gas gradients and is captured by coordinates relative to the TP (used for Figs. 5-7). The barrier effect of the TP is also relevant for convective transport (TP following coordinates also used for Fig. 7). Isentropic coordinates account for the seasonal evolution of potential temperature (θ , Fig. 4b) and best capture isentropic transport (used for Fig. 3, but also for the supplementary 5-year equivalents to Figs. 5-7).

Tracer-tracer relations in September 2012
The distribution of points in a tracer-tracer diagram provides hints on the origin and evolution of air masses. A short primer for the interpretation of such diagrams is provided in the Supplement.

Selected tracers
Here we focus on CO versus O 3 and HCl versus O 3 (Fig. 8) as well as on NO x versus O 3 and NO x versus NO y (Fig. 9).
O 3 mixing ratios in the TL exhibit a strong vertical gradient, increasing from the troposphere to the stratosphere. Given a chemical lifetime of the order of weeks, this reflects the degree of mixing between O 3 -poor UT air and O 3rich air from the lowermost stratosphere (Sprung and . That general picture might not hold in the ASMA though, where -depending on the availability of precursors -Atmos. Chem. Phys., 18, 5655-5675, 2018 www.atmos-chem-phys.net/18/5655/2018/  enhanced photochemical O 3 production is superimposed on isentropic in-mixing from the stratosphere. Enhanced CO is a tracer of boundary layer pollution and an O 3 precursor in the troposphere. Oxidation with the hydroxyl radical (OH) prevails under stratospheric conditions, and CO mixing ratios decrease by about an order of magnitude across the tropopause (Hoor et al., 2002).
As a tracer for stratospheric air we use HCl (Marcy et al., 2004;Park et al., 2008), which in the UT has no significant photochemical sources but has a lifetime similar to O 3 . Wet scavenging in clouds effectively prevents convective transport of HCl to the UT, and no injections of HCl from volcanic activity affected the ESMVal flight from Male to Larnaca. Together this makes HCl a viable tracer of stratospheric O 3 entrainments, until it is selectively removed by wet scavenging. NO x (NO + NO 2 ) is an O 3 precursor and part of NO y . NO x primarily characterises fresh emissions. Only NO was measured during the HALO ESMVal campaign, but daytime NO is a good proxy for NO x in the UT (Seinfeld and Pandis, 2006). In the UTLS, enhanced NO y originates both from tropospheric and stratospheric sources. Thus it is not a viable tracer for stratospheric air on its own. In the lower tro- posphere odd nitrogen species are co-emitted with carbon monoxide in combustion processes. Lightning and aircraft emissions are sources in the UT. Photolysis of N 2 O peaks at about 30 km and is the principal source of NO x in the stratosphere, resulting in increasing mixing ratios of NO x and NO y above the TP (Seinfeld and Pandis, 2006).

Ranges covered by observed and simulated tracer-tracer distributions
In order to place the observed tracer-tracer relations into context, we plot the measured samples together with gridcell samples from the EMAC simulation. Simulation output along the flight track is too sparse for a meaningful comparison (10 s resolution of measurements versus 12 min for the simulation). Therefore 5000 simulated samples per panel are chosen randomly, from the entire month of September 2012 and from throughout the ASMA region ( Fig. 2 Figure 9. As in Fig. 8, but focusing on reactive nitrogen. Panels (c) and (f) show NO instead of NO x , because only NO was measured. In the daytime, i.e. at the time of the measurements, NO is good proxy for NO x . The legend from panel (a) also applies to (d), and the legend from (f) applies to (c). 50 above the TP to 100 hPa below it in the actual EMAC tropopause (Fig. 8a, d) provides a zoomed-out view of possible tropospheric and stratospheric tracer mixing ratios and tracer-tracer relations for the time of year and region of the measurements. Zooming-in to the altitude range of measurements, we choose tropospheric tracers from the pressure altitude range 200 to 100 hPa (Fig. 8b, e). The observations from the entire flight without ascent and descent are shown in (Fig. 8c, f). Measurements south of the ASMA are marked by darkblue dots in Fig. 8c, f and are clearly distinct from the measurements in the ASMA filament (orange boxes). The ranges covered by the measurements are also given in the corresponding panels with simulated data, but are adjusted for model biases there. Those biases were estimated according to visual comparisons of measured versus simulated trace gas mixing ratios along the flight track in the ASMA filament (shown in the accompanying paper). All measured ranges fit into the simulated monthly averages for September 2012 in the ASMA region; thus the simulation captures this aspect well and the measurements are unlikely to represent an exceptional situation. We also note that all measurements clearly fall into the tropospheric regions of the respective simulated tracer-tracer spaces. This is no surprise: all HALO ESMVal measurements considered here were taken well within the troposphere.
Simulated O 3 and NO x increase in the stratosphere with a higher O 3 / NO x ratio than in the troposphere (Fig. 9a). However, since the range covered by the HALO ESMVal measurements is just at the intersection of the stratospheric and tropospheric branches (orange box in Fig. 9a), this does not help to distinguish the stratospheric influence from tropospheric in situ production.

In situ photochemistry, tropospheric and TL contributions
The colour code of the observations (Fig. 8c, f) corresponds to measurement time. Similar colours indicate spatial and temporal proximity, a prerequisite for mixing lines. Schematic lines L1-L5 (Fig. 8b, e) and their parallels indicate special, hypothetical cases for the evolution of air masses, which are discussed next.

CO versus O 3 (Fig. 8a-c)
O 3 and CO display opposite gradients across the tropopause and globally have lifetimes of several months in the UT (IPCC, 2013). Thus mixing lines in a CO versus O 3 scatter plot are generally suited to identifying stirring and mixing processes in the UT that occur on timescales of days to weeks, including cross-tropopause mixing (Fischer et al., 2000). The well-known L-shape (Hoor et al., 2002;Pan et al., 2004;Müller et al., 2016) is reproduced by the simulation in the CO vs. O 3 diagram for the UTLS (Fig. 8a), consisting of a CO-poor and O 3 -rich stratospheric branch connected by UTLS mixing lines to a CO-rich and O 3 -poor tropospheric branch. However, the above studies (Hoor et al., 2002;Pan et al., 2004;Müller et al., 2016) focused on the extratropics. The ASMA is mostly situated in the tropics, where trace gas mixing ratios are controlled by different processes (Gettelman et al., 2011). The ASMA in particular constitutes a special atmospheric situation, because a continuous resupply of rapidly uplifted lower-tropospheric air impedes the UT photochemical equilibrium there. O 3 is photochemically produced in the ASMA at a net rate of almost 4 nmol mol −1 day −1 and Fig. 7b, which will be discussed in Sect. 6). Only 2 weeks are needed to increase O 3 mixing ratios by 50 nmol mol −1 , i.e. to produce the O 3 enhancement observed at the southern ASMA edge. This is not much longer than the advection timescale (∼ 10 days) discussed in the context of the HALO ESMVal campaign. Thus photochemical production needs to be considered an alternative to stratospheric in-mixing to explain enhanced O 3 in the ASMA. Photochemical ageing increases O 3 and depletes CO here.
Mixing lines with negative slopes in CO vs. O 3 space dominate the UT observations (black dotted in Fig. 8c). These types of mixing lines in the troposphere could result from one or a combination of the following: (i) mixing between stratospherically and tropospherically influenced air masses, (ii) mixing between photochemically aged and freshly uplifted lower-tropospheric air and (iii) an O 3 -depleting photochemical regime (Baker et al., 2011). While the latter is unlikely in the ASMA (Fig. 7b), we need to consider additional tracers to disentangle stratospheric influence and photochemical ageing.

HCl versus O 3 (Fig. 8d-f)
HCl is a proxy for stratospheric entrainment and CO marks tropospheric influence. Consider the hypothetical case of constant HCl (lines L1 and parallels in Fig. 8b, e): increasing O 3 corresponds to increasing CO. The trace gas gradients along that hypothetical line reflect a gradient in net O 3 production rather than differences with respect to stratospheric influence between the two reservoirs. Now consider the opposite case, i.e. constant CO (lines L2): increasing O 3 corresponds to increasing HCl, indicating a gradient of stratospheric influence. CO mixing ratios decrease for increasing HCl in the special case of constant O 3 and different HCl mixing ratios (lines L3). This indicates mixing between a tropospheric and a stratospheric reservoir, where two opposite effects lead to almost constant O 3 mixing ratios: increased net O 3 production in the air with decreased HCl versus both increased O 3 and HCl in the more stratospheric components. In intermediate cases the trace gas gradients in the tracer-tracer plots reflect a combination of gradients of in-mixing as well as in situ photochemistry. Spatial gradients of photochemical The measurements (Fig. 8c, f) mostly -but not exclusively -show the latter case (L5): neighbouring points form negatively sloped lines in CO vs. O 3 space (black dotted in Fig. 8c), corresponding to horizontal to positively sloped lines in HCl vs. O 3 space (black dotted lines in Fig. 8f). Thus, observed trace gas gradients are mostly due to gradients of stratospheric influence on some well-mixed UT background. This could either be the entrainment of tropospheric air into a more stratospheric background or the entrainment of TL air into a more tropospheric background. There are also a few almost vertical mixing lines in Fig. 8f, indicating case L3 described above. Systematic HCl gradients -like those across the tropopause -are not expected in convectively uplifted air. O 3 variability in such air masses is at least partly due to different amounts of in situ produced O 3 . However, mixing between aged and young tropospheric air alone cannot explain the observations.
We further note that mixing lines in Fig. 8f cover similar ranges of HCl, but are separated by different levels of O 3 . The corresponding background air had seen similar amounts of stratospheric influence, but different O 3 production. As long as all points of an individual mixing line are subject to similar O 3 production, the entire line will be shifted to different O 3 levels. The O 3 ranges covered by individual mixing lines are similar to the offsets between different lines. Individual mixing lines in the measurements cover timescales of about 20 min (Fig. 8c), corresponding to 300 km at typical HALO speeds. The flight track in the ASMA filament covers more than 3000 km altogether and multiple mixing lines were found on that scale.
To summarise, our observations of O 3 , HCl and CO in an ASMA filament show that (i) both photochemical production and TL/stratospheric in-mixing contribute to increased O 3 in the observed ASMA filament, and (ii) small-scale gradients of stratospheric influence are superimposed on background regions that are rather homogeneous on small scales (hundreds of kilometres), but differ in their amounts of photochemically produced O 3 on larger scales (thousands of kilometres). (Fig. 9a-c) Similar HCl mixing ratios are simulated throughout the ranges of measured NO x and O 3 (orange box in Fig. 9b). Measurements of increased NO x in combination with increased O 3 (upper right corner of the orange boxes in Fig. 9) are compatible with both increased in situ O 3 production and influence from the stratospheric branch. Consequently, NO x and O 3 are well correlated on the scale of our ASMA measurements (Fig. 9c). NO x versus NO y (Fig. 9d-f): There are three distinct regions in Fig. 9d: a blueish stratospheric branch, a dark TL branch and a reddish UT region. As a consequence of the local NO y minimum directly above the tropopause ( Fig. 6d; examples of individual profiles in the Supplement), the most decreased NO y mixing ratios in Fig. 9d also show up in samples taken from near the tropopause. Measured NO and NO y values in the ASMA filament are well correlated (Fig. 9f), which is consistent with almost constant NO x / NO y ratios in the UT (Fig. 6e, f). The narrow, linear distribution of the ASMA measurements in Fig. 9c, f can be explained by different amounts of lightning NO x of approximately the same age.

Simulated intra-annual variability of trace gas dynamics in the monsoon region
In this section we discuss the evolution of simulated trace gas profiles throughout the year 2012, separately for lateral averages over the western (Iranian) and eastern (Tibetan) ASMA regions (Fig. 2).

Ozone
Steep vertical gradients across the tropopause dominate O 3 profiles in the monsoon regions (Fig. 5a, b), but the profiles also show temporal fluctuations on various timescales. Note that our lateral averaging regions are rather large, and smaller-scale structures get smoothed out, e.g. when an O 3poor interior is combined with an O 3 -rich fringe. There is increased influx from the stratosphere in spring, enhancing O 3 in the UT. This is in accordance with the study by Cristofanelli et al. (2010), but in contrast to their study there are non-negligible O 3 enhancements connected to the stratosphere during the monsoon season (Fig. 5b, circled). In this respect our simulation is, however, consistent with trace gas budget considerations for the ASMA  and the TTL (Konopka et al., 2010). Entrainment from the TL rather than deep from within the stratosphere could reconcile the different findings. No other stratospheric contributions were found for the stratospherically influenced trace gas signatures in the HALO ESMVal ASMA observations.
Enhanced O 3 is recognisable in the averaged profiles of the eastern ASMA part only from the tropopause to about 200 hPa below the tropopause, while the mid-troposphere in the Tibetan part is dominated by particularly O 3 -poor air during the monsoon season (Fig. 5b). The latter is consistent with the findings of Safieddine et al. (2016). O 3 depletion in the mid-troposphere of the eastern part is contrasted by enhanced O 3 in the mid-troposphere during the monsoon season in the western part (Fig. 5a, circled), marking the wellknown summertime O 3 maximum there.

Carbon monoxide
This is reflected in the evolution of CO profiles in the ASMA region in 2012 (Fig. 5c, d). CO-poor air dominates in the UT during spring, consistent with the stratospheric influx indicated by O 3 .
CO-rich air rises throughout the troposphere of the eastern part during the monsoon season (Fig. 5d, circled). On the western side there is a conspicuous CO-depleted zone 300 to 500 hPa below the tropopause during the monsoon season (Fig. 5c, circled), while CO is episodically enhanced in the UT. Uplifted air with enhanced CO mixing ratios hardly reaches higher than 450 hPa below the tropopause in summer.
This difference between CO profiles in the Tibetan and the Iranian parts is consistent with the findings of Pan et al. (2016). Occasional horizontal transport in the UT from the eastern to the western part of the ASMA is a possible explanation for the spatio-temporal evolution of CO mixing ratios, indicating that trace gas signatures in the Iranian part are dominated by the UT outflow of the Tibetan part of the ASMA.

Hydrochloric acid
As expected for a stratospheric tracer, the simulated HCl profiles (Fig. 5e, f) show a strong anti-correlation with CO in the UT, with increased HCl in times of stratospheric influx (e.g. Fig. 5f, blue circle) and decreased HCl in the monsoon season. Stratosphere-to-troposphere exchange is pronounced during spring, consistent with the seasonality of the Brewer-Dobson circulation (Holton et al., 1995).
HCl plumes in the Iranian part rise to about 400 hPa below the tropopause in summer (Fig. 5e, circled), just like CO. Predominantly dry conditions in the western part prevent HCl from being washed out. However, CO and HCl are temporally anti-correlated in the mid-troposphere. Since HCl is emitted by the sea, we attribute this to alternating marine and continental origins in the uplifted air (Fig. 5c, e). Some HCl descends from the tropopause into the midtroposphere, as indicated by tilted patterns of enhanced HCl, which start at the tropopause and propagate downward (marked by an arrow in Fig. 5e). Similar telltale signs of descent is also recognisable in other species in the Iranian part during summer.
There is almost no HCl in the Tibetan part throughout the monsoon season (Fig. 5f, black circle), except for the UT. Convection and thunderstorms are frequent during the monsoon season in South Asia (Fig. 7d). Wet scavenging and subsequent washing out by precipitation does not affect CO, but effectively prevents transport of HCl to higher altitudes. Predominantly continental origins also contribute to an increased CO / HCl ratio in the rising plumes of the eastern part.

Reactive nitrogen
Simulated NO x and NO y profiles in the ASMA region from April to September differ to the rest of the year (Fig. 6ad). E-and C-shaped NO y profiles dominate the Tibetan and Iranian parts, respectively (Fig. 6c, d; examples of individual profiles in the Supplement). NO x and NO y from boundary layer sources are uplifted, accompanied by conversion of some NO x into NO y . Solvable NO y components (e.g. HNO 3 ) become increasingly washed out (Fig. 6d), leading to a minimum of reactive nitrogen in the mid-troposphere in the Tibetan part in summer (Fig. 6b, d). Uplift from the lower troposphere is less important for UT NO x and NO y than LiNO x and stratospheric entrainments. The dependence of detrainment on altitude hardly affects trace gas profiles in the mid-troposphere, as indicated by the corresponding CO profiles (Fig. 5d, circled).
Both NO x and NO y gradually increase above the tropopause due to stratospheric photochemistry. Stratospheric influx contributes to increased NO x mixing ratios in the UT in spring (blue circles in Figs. 5f, 6b), but enhanced UT NO x during the monsoon (Fig. 6b, black circle) is more due to lightning NO x emissions in the Tibetan part than to stratospheric entrainments (Supplement).
NO y can rise to about 400 hPa below the tropopause in the heat low over the Arabian Peninsula (circled in Fig. 6c). Downward transport (as indicated by anti-clockwise tilted signals, one example marked by an arrow in Fig. 6c) dominates above that altitude, preventing further uplift. With little in situ production of lightning NO x over the Arabian Peninsula in summer (Figs. 7c and 10), UT NO y in the Iranian part is dominated by the outflow of the Tibetan part.
As a combination of the different processes affecting NO x and NO y , the NO x / NO y ratio maintains a broad maximum in the TL throughout the year (Fig. 6e, f). During the monsoon, the NO x / NO y ratio in the UTLS is larger in the western than in the eastern ASMA part (Fig. 6e, f, circles). This indicates preferential export of high-NO x air from the Tibetan part or is an artefact of the possible dominance of a single source of LiNO x in the Iranian region (Fig. 10).

Processes and their interplay in the ASMA
In this section the observed and simulated trace gas signatures are related to simulated photochemical, transport and mixing properties of the ASMA. The term "interplay" is thereby used in a neutral sense regarding the direction of feedbacks between different processes: it subsumes mostly one-way interactions (e.g. emissions affecting O 3 production, dynamics affecting trace gas distributions). We note upfront that the intra-annual variability of trace gas dynamics in the Tibetan and Iranian ASMA regions discussed for the year 2012 in Sect. 5 is largely similar to the other considered years (2010-2014; shown in the Supplement).

Lightning NO x
In our EMAC simulations, LiNO x is released based on a parameterisation that links flash frequency to updraught velocity in -also parameterised -convection. It is difficult to pinpoint LiNO x emissions (Schumann and Huntrieser, 2007), and both parameterisations are a notorious source of uncertainty in global models. The parameterisations for convection (Tiedtke, 1989;Nordeng, 1994;Tost, 2006) and lightning (Grewe et al., 2001) used in our simulations have been tested in several studies (Tost et al., 2007;Grewe, 2009;Lopez, 2016) and appear to be state of the art. EMAC-simulated lightning activity matches the corresponding TRMM-LIS/OTD (Tropical Rainfall Measuring Mission Lightning Imaging Sensor/Optical Transient Detector) observations (Cecil, 2006) reasonably well, spatially and temporally (Supplement). Simulated and observed NO along the HALO ESMVal flight track agree remarkably well within the ASMA region (accompanying paper). The same is true for comparisons of IAGOS-CARIBIC measurements of NO and our simulation's output along the IAGOS-CARIBIC flight tracks, where the agreement is particularly noticeable for the monsoon season in the ASMA region (Supplement). A ded-icated comparison to other models is still desirable, since NO x is complex to simulate and there might be compensating errors. For the current study, however, the above comparisons provide some confidence that LiNO x emissions have been captured well by the simulation.
Simulated LiNO x emission rate profiles for 2012 show prominent maxima for the eastern and western ASMA regions during spring (Fig. 7c, d). Overall, LiNO x emissions are much stronger in the Tibetan part. The emissions reach up to the tropopause throughout the year, implying that LiNO x is emitted at higher potential temperatures during the monsoon season (Fig. 4b). Despite higher emission rates in the laterally averaged profiles (Fig. 4d), lightning activity in the Tibetan part is more sporadic and localised in spring than in summer (Fig. 10d, e). During the monsoon season, LiNO x is constantly replenished in the ASMA throughout the region (Fig. 10g, h, i). Sensitivity simulations show that UT NO x (Fig. 6b) is mainly LiNO x during the monsoon season (Supplement).

Entrainment of lower-tropospheric air
The uplift of lower-tropospheric air to the UT is a wellknown characteristic of the ASMA . Simulated CO profiles in the Tibetan region show episodes of such uplift, not only for 2012 (Fig. 5d), but for every mon- soon season during . This is consistent with the HALO ESMVal measurements, since the trace gas gradients observed in the ASMA can be explained by mixing between lower-tropospheric air and stratospherically influenced air. CO uplift to the UT and LiNO x emissions are both related to convection and it is remarkable that there is a much stronger correlation between the two in summer than in spring (Figs. 5d, 7d). We attribute this to three effects: (i) the large-scale uplift at the south-western flank of the Himalayas is only active during the monsoon season and is not exclusively driven by deep convection (see Sects. 1, 3). It has been suggested to be the main transport pathway of pollutants to the UT (Bergman et al., 2013;, which is supported by our simulation (Fig. 11) and the location of maximum moist static energy (Boos and Hurley, 2013). Back-trajectory calculations in the accompanying paper identified this pathway as the source of enhanced CO in some of the HALO ESMVal measurements, despite the underlying reanalysis not accounting for (small scale) convection. (ii) In the UT the ASMA is a leaky transport barrier, allowing some accumulation of the uplifted pollutants . There is no such transport barrier in spring. (iii) The spatial and temporal matches of deep convection and increased CO at different altitudes reflect the potential for entrainment and subsequent convective transport of CO (Fig. 7g, h). It is clearly increased in summer. More detailed analyses (Supplement) show that convection is localised over the coastal regions of West Bengal and Bangladesh in April 2012. In contrast, during August 2012 convection is ubiquitous throughout the Tibetan region. It is most persistent at the south-western flank of the Himalayas and over the Tibetan plateau. This coincides with the highest CO mixing ratios, which accumulate there due to the prevalent south-westerly winds during the monsoon season. Con-sequently, more CO is transported through the troposphere in the Tibetan region during summer.

Photochemical O 3 production and ageing
The net photochemical O 3 production rate (Fig. 7a, b) is derived from the difference between EMAC-simulated diagnostic tracers ProdO 3 and LossO 3 (Jöckel et al., 2016). Here we take into account effective O 3 production and loss terms following Crutzen and Schmailzl, (1983) and extended by Grewe et al. (2017;see their Supplement). There are known high-O 3 biases in the simulation (Jöckel et al., 2016), and uncertainties in the chemical mechanism (Gottschaldt et al., 2013) also impose uncertainties onto O 3 photochemistry. Nevertheless our simulated net O 3 production rates in the ASMA (Fig. 7b) agree remarkably well with the independent estimate by Barret et al. (2016).
O 3 photochemistry is dominated by catalytic cycles in the troposphere and affected by a variety of parameters, e.g. ambient mixing ratios of H 2 O, O 3 , CO and NO x (Ehhalt and Rohrer, 1994;Grooß et al., 1998;Jaeglé et al., 1998;Seinfeld and Pandis, 1998). We focus on NO x and CO for illustration (Fig. 12). Photochemical O 3 production 1 (ProdO 3 ) non-linearly depends on ambient NO x mixing ratios: it increases proportional to NO x in the NO x -limited regime, is almost independent of NO x variations at higher NO x mixing ratios, and a further increase of NO x even leads to decreasing ProdO 3 (NO x -saturated regime). Increasing CO increases ProdO 3 and shifts the point of maximum ProdO 3 to higher NO x . Increasing H 2 O impacts ProdO 3 in a qualitatively similar way to increasing CO. Decreasing O 3 leads to higher ProdO 3 , but NO x at the point of maximum ProdO 3 is at its lowest for medium O 3 mixing ratios.
The simulation shows the superposition of the above effects, among others within the full complexity of the chemical mechanism. As a result, a net O 3 -producing photochemistry prevails in the ASMA throughout the monsoon season (circled in Fig. 7a, b). This is accompanied by net O 3 destruction during the monsoon season, 300 hPa below the tropopause and lower. At the tropopause and slightly above, there is a local minimum of net O 3 production, followed by increased net O 3 production in the stratosphere. Net O 3 production is at maximum in the altitude range, where uplifted young air (enriched in CO and co-emitted volatile, organic O 3 precursors) mixes with NO x -rich UT air (Figs. 5d, 6b,  7b).
ProdO 3 per NO x shows a strong gradient at the altitude of maximum net O 3 production (circled in Fig. 7b, f). This indicates the transition from the NO x -limited to the NO xsaturated regime (Fig. 12), but is superimposed by gradients of CO and other O 3 precursors. The maximum corresponds to about 300 pmol mol −1 NO x (circled in Fig. 8h), and vari- Figure 12. Schematic of the dependence of photochemical O 3 production (ProdO 3 ) on NO x and CO mixing ratios (after Grooß et al., 1998). Red, green and blue highlight photochemical conditions that are discussed in the text. Approximate numbers (Ehhalt and Rohrer, 1994;Jaeglé et al., 1998;Grooß et al., 1998) for UT conditions at northern midlatitudes the point of maximum O 3 production may vary between 200 and 700 pmol mol −1 NO x . The maximum net O 3 production varies by a factor of about 4, depending on ambient conditions. ations of NO x in that region have a relatively small effect on net O 3 production (2 in Fig. 12).
Going down from the TP in the ASMA, NO x and O 3 generally decrease, while CO and H 2 O increase (Figs. 5, 6; H 2 O not shown). It is a multi-dimensional problem. CO (among others) determines the curve in the NO x vs. ProdO 3 diagram, and NO x determines the operating point on the curve. Considering typical ranges of CO and NO x in different parts of the ASMA, an area on the surface in ProdO 3 -NO x -CO space is termed "operating mode of the chemical system" in the following. Different chemical regimes (e.g. NO x -limited or NO x -saturated) are allowed within one operating mode. The non-linear dependence of ProdO 3 on ambient trace gas mixing ratios leads to the simulated maximum within the opposite gradients of those trace gases (NO x decreases below the TP, while CO increases) in the UT ASMA. Going down from the TP, the chemical system goes from operating mode 3 to 2 to 1 (Fig. 12). In principle, all those operating modes could be in the NO x -limited regime and still lead to a maximum of net O 3 production in the UT. However, our simulations also show the NO x -saturated regime (Supplement).
Periods of enhanced lightning NO x in spring (circled in Fig. 7d) correspond to increased net O 3 production (Fig. 7b), but despite higher LiNO x emissions in spring, net O 3 production is at maximum in the ASMA. The main differences between the seasons are that there is less CO in the UT during spring (Fig. 5d) and lightning NO x is available only locally (Sect. 6.1. and Supplement). More CO in the UTLS in summer increases ProdO 3 and the maximum possible O 3 production (Fig. 12). Too high NO x in spring does not help ProdO 3 -or even pushes the system into the NO x -saturated regime (3 in Fig. 12). NO x close to maximum ProdO 3 conditions (2 in Fig. 12) throughout the region in summer leads to higher ProdO 3 in the lateral average.
Both NO x and other precursors are more abundant in the UT of the Tibetan part, resulting in larger photochemical O 3 production than in the Iranian part (Fig. 7a, b). This is consistent with other studies (J. J. , which have also found such an asymmetry. O 3depleting conditions prevail in the mid-troposphere over the Arabian Peninsula throughout the summer (Fig. 7a, circled). Thus increased O 3 there (Fig. 5a) must be due to transport.
Confinement in the ASMA circulation allows the mixed air to age, i.e. to produce O 3 . CO is being depleted in the process of ageing, and NO x is transferred to NO y . The other source of aged air is entrainment from the TL, which is, however, enriched in HCl (at least within the photochemical lifetime of HCl). O 3 is produced in the ASMA at a net rate of about 4 nmol mol −1 day −1 (Fig. 7b), and simulated O 3 mixing ratios in the UT of the ASMA region vary by about 120 nmol mol −1 (Fig. 8b). It would take 30 days to cover that range by photochemical O 3 production alone. The observed values in the ASMA filament cover a range of about 48 nmol mol −1 (Fig. 8c), corresponding to 12 days of photochemical O 3 production. According to the trajectory calculations in the accompanying paper, this is about the time needed to circle the ASMA. The above O 3 variability of course includes different amounts of O 3 from the TL, and O 3 productivity varies too. Neglecting these uncertainties, it takes one or two rotations of the ASMA to transform O 3depleted, freshly uplifted air into aged, O 3 -enhanced air. O 3depletion in the ASMA relative to the regional average can only be maintained by frequent replenishment of young air.

Entrainment of tropopause layer air
Here we focus on the less well-known entrainment of stratospheric or TL air into the free troposphere, which is supported by the unique thermodynamic conditions over the Tibetan plateau in summer (Fig. 2). The prevailing northerly winds (Kunze et al., 2010) of the eastern ASMA flank (Fig. 2) tend to transport high potential vorticity (stratospheric or TL, Fig. 4c) air along the isentropic surfaces into the troposphere (Ren et al., 2014;Kunz et al., 2015). This effect was also detected by Konopka et al. (2010) as enhanced horizontal transport of O 3 -rich air from the extratropics into the TTL. This transport from the TL or even the extratropical lower stratosphere into the free tropical troposphere may not leave a telltale sign of increased potential temperature in the corresponding air masses in the tropics. This includes the 350-370 K isentropes that were encountered during the HALO ESMVal campaign in the tropics ( Fig. 4; θ estimates for the measurements are shown in the Supplement).
Additional stratospheric or TL contributions at the outer ASMA edge, other than at the eastern flank, are also plausible. The eastern Mediterranean and central Asian region is a global hotspot of tropopause-folding activity (Tyrlis et al., 2014), which is related to ASMA dynamics and generates enhanced O 3 levels through stratosphere-troposphere exchange (Akritidis et al., 2016). If the ASMA circulation encompasses that tropopause folding hotspot, it may pick up stratospheric entrainments.
Stratospheric influence is manifested in our measurements by increased HCl mixing ratios in combination with other tracers (Sect. 4.3).
Did the HALO ESMVal campaign encounter an exceptional situation, or does TL entrainment at the eastern ASMA flank occur more often? The synoptic situation in question is characterised by a filament of enhanced HCl that is carried along the south-eastern ASMA flank, around a HCl-depleted ASMA interior. Here we analyse the evolution of simulated HCl mixing ratios at θ = 355 K, on a meridional (N-S) transect at 90 • E, throughout the monsoon seasons of 2010 to 2014. The transition between eastward and westward winds indicates the location of the ASMA centre on the meridional transect, which wobbles around 30 • N (white "ridgeline" in Fig. 3b). Enhanced tropospheric HCl mixing ratios south of the ridgeline serve as an indicator of TL entrainment (Fig. 3c). Caution with this interpretation is only needed at times when the ASMA is shifted to the west (compare Fig. 3a), because the transect in Fig. 3c may then be too far within the eastern ASMA flank. Episodes of increased HCl in the southern or eastern ASMA flank cover at least half of the time axis, showing that entrainment of TL air into the ASMA circulation is quite a common process. One horizontal slice from each analysed month is shown in the Supplement, indicating that filaments of enhanced HCl often protrude from a TP trough of a Rossby wave at the eastern ASMA flank. The association of this mixing process with planetary wavebreaking events is a topic of ongoing research (Lubis and Nakamura, 2017).

Radial stratification and patchy trace gas distributions
Deep convection from the lower troposphere discharges more towards the ASMA interior, as shown by studies that report relatively young air there (Li et al., 2005;Randel and Park, 2006;Park et al., 2008;Y. Liu et al., 2009;Kunze et al., 2010;Liu et al., 2011;Santee et al., 2017) and also by our simulation (Sect. 6.4). In contrast, trace gas signatures in a belt of outer streamlines are dominated by a combination of photochemically aged lower-tropospheric air and entrainments of UT air surrounding the ASMA. In this schematic of an undisturbed anticyclone, interior trace gas signatures are generally characterised by lower O 3 mixing ratios than fringe signatures. This radial zoning in the ASMA is an expression of almost closed circulation and was observed in IAGOS-CARIBIC in situ data of flights between Chennai, India and Frankfurt, Germany (Baker et al., 2011;. Increased O 3 mixing ratios were found in the northern part of the ASMA and decreased levels towards the southern end of the flights. Radial stratification is counteracted by the general on-off nature of TL entrainment, upwellings from the lower troposphere and lightning. Still considering only undisturbed ASMA circulation, all those effects lead to patches of air with different trace gas signatures. Each of these patches might again receive contributions from any of the above sources. In principle all sorts of combinations are possible, generating heterogeneity. In contrast, mixing and photochemical ageing are homogenising effects. In combination with closed streamlines the preferential positions of the different sources might still show up as radial stratification in the ASMA, or show up in individual situations (Sect. 6.4).
However, neither the HALO ESMVal measurements nor sequences of simulated snapshots (Supplement) show clear stratification. The idealised picture that the ASMA circulation is dominated by stationary, closed streamlines is certainly not realistic -at least not on the timescales of the homogenising effects.

Splitting-up and stirring
Transient streamlines, particularly eddy shedding or splitting of the ASMA, effectively overcome radial transport barriers. Whether stratified or patchy -any trace gas distribution in the ASMA might then be subject to effective stirring. There is an ongoing discussion about different dynamical modes of the ASMA .
A splitting-up event occurred during the HALO ESMVal campaign, corresponding to the transition from a longitudinally elongated phase to a double centre phase in the nomenclature of . A sequence of simulated streamlines and tracer distributions shows that parts of the fringe of the elongated anticyclone become part of the interiors of both resulting anticyclones after the splitting, and the interior parts are diverted into the fringes (Fig. 13). Even if not all possible cases are covered by the example, it is easily conceivable that the some or all of the fringing parts may stay in the fringes and some or all of the interior parts in the interiors. For a given location and timing of eddy shedding or splitting, the final trace gas distribution simply depends on the initial distribution of different patches. The redistribution of different parts of the anticyclone guarantees a high variability for outflow and interior, whenever the closed circulation breaks down.
How often does this happen? Splitting and eddy shedding mainly occur in a zonal (E-W) direction, whereby the transition from a northward wind in the west to a southward wind in the east indicates the centre of an anticyclone or eddy. We analyse the evolution of meridional winds at θ = 355 K, on a wide (15-35 • N) zonal transect, throughout the monsoon seasons of 2010 to 2014 (Fig. 3a).
The pattern at the given altitude is consistent with one dominating anticyclone, centred at about 90 • E. While the  Figure 13. Sequence of simulated tracer fields at 355 K, illustrating the stirring associated with the splitting-up event of the ASMA that occurred during the HALO ESMVal campaign in September 2012. Streamlines (grey) represent instantaneous wind fields, and arrows highlight the redistribution of selected air masses. CO mainly originates in the ASMA interior and HCl serves as a proxy with which to track the ASMA fringe. The sequence starts with an elongated anticyclone on 16 September 2012. Then a tropopause trough (T) evolves from the west along the northern ASMA flank. The anticyclone succumbs to the perturbation and splits up into a Tibetan and an Iranian part, shortly after the HALO flight from Male to Larnaca had passed through. A part of the increased CO interior region is entrained by the outer streamlines of the Iranian part, while the rest of the patch is diverted into the interior of the Tibetan anticyclone (black arrows in the left panels). The evolution of freshly entrained HCl (black arrows) and an older patch (red arrows) are shown in the right panels. We also note entrainment of tropospheric air by southerly winds at the western flank (white arrows).
northerly winds east of 90 • E are relatively persistent, episodes of entirely southerly winds in the western part of the one-piece ASMA alternate with episodes of smaller, secondary anticyclones. Smaller anticyclones also regularly occur east of the Tibetan anticyclone, corresponding to eddy shedding to the east. The splitting event that occurred during the HALO ESMVal campaign is clearly visible in Fig. 3a, too. Such instabilities occur approximately twice a month. This coincidentally corresponds to the timescale needed to photochemically erase O 3 -depleted signatures in young air masses.

Summary
This study complements a detailed analysis of in situ trace gas measurements in the ASMA, obtained during the ESM-Val campaign with the research aircraft HALO in September 2012 (Gottschaldt et al., 2017). The measurements are put in the context of the EMAC-simulated annual evolution of trace gas profiles in the ASMA region and simulated tracer-tracer relations. This led to the following qualitative understanding of the interplay of processes that determine the trace gas dis-tributions in the ASMA and its outflow (Fig. 14): Air from the steeply inclined TL is entrained by outer ASMA streamlines at the eastern and possibly northern ASMA flank, defining a fringing zone. Tropopause troughs facilitate the entrainment. Stratospherically enhanced tracers like HCl and O 3 are reflected in the entrained air. Thus, the fringe is not just a transport barrier, separating the ASMA interior from the surrounding UT. It has a distinct genesis, resulting in air masses with distinct trace gas signatures that may be transported relatively unperturbed over long distances. Deep convection and a conduit of upwelling air over the Tibetan plateau (Bergman et al., 2013) inject lower-tropospheric air mainly into the Tibetan part of the ASMA. Enhanced CO is an indicator for this process. Convection is accompanied by in situ production of lightning NO x , mainly determining mixing ratios of this O 3 precursor in the ASMA.
In the idealised case of one intact anticyclone (Fig. 14a) the interior would then be dominated by photochemical ageing of those O 3 -poor injections. Net O 3 production dominates in the ASMA and is particularly enhanced where mainly lower-tropospheric O 3 precursors (CO, volatile or- ganic compounds) meet UT precursors (NO x ). The preferential positions of convective versus TL entrainments facilitate radial stratification in the ASMA. The intermittent nature of the entrainments, combined with the varying position of the anticyclone, leads to patches of air that have different origins and are in different stages of ageing. Mixing and ageing are homogenising, but each of these patches might again receive fresh entrainments from the TL or by convection and lightning.
Eddy shedding or transitions between other dynamical modes of the ASMA effectively overcome radial transport barriers (Fig. 14b, summarising Figs. 13 and S18 in the Supplement). Whether stratified or patchy, any trace gas distribution in the ASMA is subject to effective stirring. Fringe air can be diverted into the interiors of both anticyclones, and likewise interior air is redistributed throughout the UT in the monsoon region. Remnants of earlier such events gradually lose memory of their origins, leading to a mixed background (grey in Fig. 14b).
We found that the processes that led to the curious combination of both enhanced lower tropospheric and TL tracers in the ASMA filaments encountered by the HALO ESM-Val campaign are not exceptional: entrainment of TL air and dynamical instabilities of the ASMA occur quite frequently. Deep convection and thunderstorms are common throughout the monsoon season, accompanied by a net O 3 producing photochemical regime. The alternating interplay of those processes results in highly variable, patchy trace gas distributions in the ASMA. Processes that increase O 3 and its precursors dominate in the Tibetan part of the ASMA. The Iranian part is dynamically dominated by the Tibetan part in the UT. O 3 -rich TL entrainments and precursor-rich air, both of which are main ASMA components, tend to increase O 3 in the tropospheric ASMA outflow -e.g. over the Arabian Peninsula.
Data availability. The simulation results analysed here are archived at the German Climate Computing Center (DKRZ) and are available on request. It is planned to move them to the Climate and Environmental Retrieval and Archive (CERA) database at the German Climate Computing Centre (DKRZ; https://cera-www. dkrz.de, last access: 18 April 2018). The corresponding digital object identifiers (DOIs) will be published on the MESSy consortium web page (http://www.messy-interface.org, last access: 9 April 2018). The observational data of the HALO ESMVal flight used here are available from the HALO database (re3data.org, 2018). We used the NCAR Command Language (NCL) for data analysis and to create some of the figures of this study. NCL is developed by UCAR/NCAR/CISL/TDD and available online (UCAR/NCAR/CISL/TDD, 2017).
Author contributions. KDG analysed the EMAC and final in situ data, conducted the Lagrangian calculations, produced the plots and drafted the paper. HS conceived the study, led the HALO ESMVal campaign and interpreted EMAC and in situ data. RB wrote and helped with the code that facilitated the HYSPLIT calculations. PJ led the ESCiMo project, coordinated the preparation of the EMAC simulations and conducted them. DSC and PG prepared a significant part of the boundary conditions, and VG was responsible for the ProdO 3 and LossO 3 diagnostics in the ESCiMo simulations. VE conceived and led the ESMVal project. TJW, CV, AZ and HZ supplied in situ measurements. All authors contributed to the text.
Competing interests. The authors declare that they have no conflict of interest.
Special issue statement. This article is part of the special issue "The Modular Earth Submodel System (MESSy) (ACP/GMD interjournal SI)". It is not associated with a conference.
for funding within HALO-SPP 1294 under the contracts JU 3059/1-1, SCHL 1857/2-2, SCHL 1857/4-1, VO 1504/2-1 and VO 1504/4-1. The HALO ESMVal aircraft campaign was funded by the DLR project ESMVal. Klaus-Dirk Gottschaldt and Hans Schlager appreciate support by the EU project StratoClim (grant no. 603557) and BMBF project Spitfire (grant no. 01LG1205B). Christiane Voigt and Tina Jurkat-Witschas are thankful for financing from the Helmholtz Association under contract no. VH-NG-309 and under contract no. W2/W3-60. In addition we thank the flight department of DLR for their great support during the campaign. Peter Hoor and Stefan Müller contributed to the CO measurements and Stefan Kaufmann supervised the HCl measurements during the flight.
The EMAC model simulations were performed at the German Climate Computing Centre (DKRZ) with support from the Bundesministerium für Bildung und Forschung (BMBF). DKRZ and its scientific steering committee are gratefully acknowledged for providing the HPC and data archiving resources for the projects 853 (ESCiMo -Earth System Chemistry integrated Modelling) and 854 (ESMVal).
Last but not least we thank the two anonymous reviewers for their insightful comments regarding LiNO x , convective and isentropic transport, which greatly helped to improve the paper.
The article processing charges for this open-access publication were covered by a Research Centre of the Helmholtz Association.
Edited by: Marc von Hobe Reviewed by: two anonymous referees