# Dominant Modes of Tropospheric Ozone Variation over East Asia from GOME Observations

Authors: Yi Liu; Yuli Zhang; Yong Wang; Chuanxi Liu; Zhaonan Cai; Paul Konopka; Rolf Müller
Journal: Advances in Meteorology
 (2015)

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## Abstract

The variation in tropospheric ozone over East Asia was analyzed using tropospheric column ozone data measured by the Global Ozone Monitoring Experiment (GOME) satellite. An empirical orthogonal function (EOF) analysis was carried out to derive the dominant modes of the variation in the tropospheric ozone volume-mixing ratio (TOVMR). The EOF1 mode, which explained 61.5% of the total variance, showed a same-sign distribution over all of East Asia, with a belt of enhanced ozone concentrations around 40°N. The principal component of EOF1 (PC1) suggested that photochemical ozone production together with Brewer-Dobson circulation and subtropical westerly jet plays important roles in modulating the seasonal variation of the TOVMR; ozone-rich air produced by photochemical processes was transported from the stratosphere to the troposphere by BD circulation and this ozone-rich air was then blocked by the subtropical westerly jet and accumulated north of the jet. The EOF2 mode explained 29.2% of the total variance with an opposite-sign pattern on the north and south side of 35°N. When anticyclonic circulation transported ozone-poor air from the upwelling area over the Bay of Bengal towards the Tibetan Plateau during the onset of the Asian summer monsoon, tropospheric ozone in this region decreased dramatically.


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## Body

## 1. Introduction

Tropospheric ozone has been considered a greenhouse gas for some time [1]. It has strong effects on radiative forcing [2] and is an important component of the photochemical reactions that occur in the boundary layer [3]. Increasing ozone concentrations in this layer threaten human health and surface ecosystems [4]. Therefore, studies into the spatiotemporal characteristics of tropospheric ozone and its drivers are important theoretically and practically.With the rapid development of the Asian economies in recent decades, air pollution has increased dramatically [5] and influenced atmospheric chemistry, radiation, and dynamics at regional and global scales. Some air pollutants can directly or indirectly affect ozone concentrations, by influencing the photochemical reactions that generate ozone in the troposphere. Dramatic changes in the concentrations of ozone and its precursors have caused international concern; this has inspired research, including into the effects of increasing air pollution in Asia on ozone concentrations and climate [6], extreme tropospheric ozone events [7], the production, distribution, and evolution of tropospheric ozone [8], cross-tropopause ozone fluxes over east Asia [9, 10], long-range transport of ozone in the East Asian Pacific Rim region [11], tropospheric ozone during the Asian summertime monsoon [12], and tropospheric ozone modeling over Asia [13].Recently, Randel et al. [14] suggested that tropospheric pollution could be transported into the stratosphere by the Asian summer monsoon and further influence the global atmosphere and climate. However, there are few ozonesonde stations in East Asia and long-term continuous ozone profile measurements are especially limited. Because of the lack of sufficient ozonesonde measurements, most researchers who study ozone concentrations over Asia have had to rely on satellite datasets, or limited ground-based measurements.In this study, the dominant modes of tropospheric ozone variation over Asia were investigated, using empirical orthogonal function (EOF) analysis. Tropospheric column ozone derived from satellite measurements was used to examine the mechanism (photochemistry and transport) behind this variation of the tropospheric ozone over Asia. Section2 describes the data and methods used. Section 3 describes the seasonality of tropospheric ozone. Section 4 analyzes the dominant modes of the tropospheric ozone variation and their mechanisms. Conclusions are summarized in Section 5.


## 2. Data and Methods

### 2.1. Satellite Ozone Measurements

The Global Ozone Monitoring Experiment (GOME), on board the European Space Agency (ESA) Remote Sensing-2 (ERS-2) satellite, measured radiance backscattered from the Earth’s atmosphere over a wavelength range of 240–790 nm. GOME had a moderate spectral resolution of 0.2–0.4 nm and high signal-to-noise ratios in ozone absorption bands, making it possible to retrieve the vertical distribution of ozone from the troposphere to the stratosphere [15]. The ozone profile and tropospheric column ozone (TCO) were retrieved from GOME measurements by performing extensive calibration and improvements in the Liu forward model [16–18]. Tropopause pressure reanalysis data from the National Centers for Environmental Prediction (NCEP) were used to separate the stratosphere and troposphere.The retrieved ozone profiles agreed well with measurements from ozonesonde, Total Ozone Mapping Spectrometer (TOMS), and Stratospheric Aerosol and Gas Experiment II (SAGE-II) [16, 19]. Validation with ozonesonde from 33 stations between 75°N and 71°S during 1996–1999 showed that the retrieved TCO profiles captured most of the temporal variability in ozonesonde TCO; the mean biases were mostly within 3 DU (15%) and the 1σ standard deviations were within 3–8 DU (13–27%). We compared GOME ozone profiles to ozonesonde measurements over three stations in China, including Beijing (39.8°N, 116.47°E) from September 2002 to June 2003, Lhasa (29.7°N, 91.1°E) from June to October in 1998 and 1999, and Xining (36.63°N, 101.75°E) from April to August 1996 [20]. In the middle and lower troposphere, the bias was within ±10% over Beijing and ±5% over Lhasa and Xining; in the upper troposphere and lower stratosphere (UTLS), the GOME data had biases of ±10% over Beijing and positive biases of 10% over Lhasa and 5% over Xining; in the middle stratosphere, the GOME retrievals compared well to ozonesonde values over Lhasa but had a negative bias of 10% over Xining and a positive bias of up to 20% over Beijing. The mean biases of the TCO were less than 10% over these three stations.The spatial resolution of GOME retrievals is normally 960 × 80 km2. We mapped the swath data from orbits onto a 2° latitude × 2.5° longitude grid and derived monthly averaged data for March 1996 to June 2003. The TCO was converted from Dobson units to the mean tropospheric ozone volume mixing ratio (TOVMR, in ppbv unit), using the method described by Ziemke et al. [21].


### 2.2. Definition of Westerly Jet Occurrence

The definition of westerly jet occurrence was based on the methods of Schiemann et al. [22], with the difference being that the wind data used here was in potential temperature (θ) coordinates rather than pressure coordinates. A four-dimensional index field of jet occurrence, J(t,x,y,θ), was set to either zero or one, where t, x, and y refer to time, latitude, and longitude, respectively. It was set to one when the horizontal velocity Vt,x,y,θ=[ut,x,y,θ,vt,x,y,θ] satisfied (1a)Vt,xy,θis a local maximum,(1b)V≥30ms-1,(1c)u≥0ms-1and to zero otherwise. Subscripts denote fixed dimensions; that is, J identifies the maxima of the horizontal wind speed in latitude-theta cross sections. The jet identification was carried out between 280 and 400 K, using the European Centre for Medium-Range Weather Forecasts (ECMWF) meteorological ERA-interim reanalysis [23], at time intervals of 6 hours during 1996–2003.


### 2.3. Definition of Monsoon Index

The Monsoon-Hadley index (MHI), which is based on the anomalous meridional wind shear, was used as a suitable monthly mean monsoon index to describe the intensity of the South Asian (Indian) summer monsoon circulation [24]:(2)MHI=V850∗-V200∗,where V850∗ and V200∗ are the regional and temporal mean meridional wind anomalies, at 850 hPa and 200 hPa, respectively, over the monsoon region (10°N–30°N, 70°E–110°E) during April–August.


### 2.4. Empirical Orthogonal Function (EOF) Analysis

EOF analysis decomposes the space-time field into a set of orthogonal spatial patterns along with a set of associated, uncorrelated, time indices or principal components (PCs) in a linear fashion. The EOF technique aims to find a new set of variables that capture most of the observed variance from the data, through linear combinations of the original variables, or reduce the large number of variables of the original data to a few variables. It has proven to be a powerful tool for identifying dominant modes of climate variability and tracer analysis [25]. In this study, EOF analysis was applied to the monthly mean TOVMR dataset over East Asia (80°E–140°E, 10°N–50°N) from March 1996 to June 2003 to retrieve the dominant spatiotemporal modes of tropospheric ozone over East Asia.


## 2.1. Satellite Ozone Measurements

The Global Ozone Monitoring Experiment (GOME), on board the European Space Agency (ESA) Remote Sensing-2 (ERS-2) satellite, measured radiance backscattered from the Earth’s atmosphere over a wavelength range of 240–790 nm. GOME had a moderate spectral resolution of 0.2–0.4 nm and high signal-to-noise ratios in ozone absorption bands, making it possible to retrieve the vertical distribution of ozone from the troposphere to the stratosphere [15]. The ozone profile and tropospheric column ozone (TCO) were retrieved from GOME measurements by performing extensive calibration and improvements in the Liu forward model [16–18]. Tropopause pressure reanalysis data from the National Centers for Environmental Prediction (NCEP) were used to separate the stratosphere and troposphere.The retrieved ozone profiles agreed well with measurements from ozonesonde, Total Ozone Mapping Spectrometer (TOMS), and Stratospheric Aerosol and Gas Experiment II (SAGE-II) [16, 19]. Validation with ozonesonde from 33 stations between 75°N and 71°S during 1996–1999 showed that the retrieved TCO profiles captured most of the temporal variability in ozonesonde TCO; the mean biases were mostly within 3 DU (15%) and the 1σ standard deviations were within 3–8 DU (13–27%). We compared GOME ozone profiles to ozonesonde measurements over three stations in China, including Beijing (39.8°N, 116.47°E) from September 2002 to June 2003, Lhasa (29.7°N, 91.1°E) from June to October in 1998 and 1999, and Xining (36.63°N, 101.75°E) from April to August 1996 [20]. In the middle and lower troposphere, the bias was within ±10% over Beijing and ±5% over Lhasa and Xining; in the upper troposphere and lower stratosphere (UTLS), the GOME data had biases of ±10% over Beijing and positive biases of 10% over Lhasa and 5% over Xining; in the middle stratosphere, the GOME retrievals compared well to ozonesonde values over Lhasa but had a negative bias of 10% over Xining and a positive bias of up to 20% over Beijing. The mean biases of the TCO were less than 10% over these three stations.The spatial resolution of GOME retrievals is normally 960 × 80 km2. We mapped the swath data from orbits onto a 2° latitude × 2.5° longitude grid and derived monthly averaged data for March 1996 to June 2003. The TCO was converted from Dobson units to the mean tropospheric ozone volume mixing ratio (TOVMR, in ppbv unit), using the method described by Ziemke et al. [21].


## 2.2. Definition of Westerly Jet Occurrence

The definition of westerly jet occurrence was based on the methods of Schiemann et al. [22], with the difference being that the wind data used here was in potential temperature (θ) coordinates rather than pressure coordinates. A four-dimensional index field of jet occurrence, J(t,x,y,θ), was set to either zero or one, where t, x, and y refer to time, latitude, and longitude, respectively. It was set to one when the horizontal velocity Vt,x,y,θ=[ut,x,y,θ,vt,x,y,θ] satisfied (1a)Vt,xy,θis a local maximum,(1b)V≥30ms-1,(1c)u≥0ms-1and to zero otherwise. Subscripts denote fixed dimensions; that is, J identifies the maxima of the horizontal wind speed in latitude-theta cross sections. The jet identification was carried out between 280 and 400 K, using the European Centre for Medium-Range Weather Forecasts (ECMWF) meteorological ERA-interim reanalysis [23], at time intervals of 6 hours during 1996–2003.


## 2.3. Definition of Monsoon Index

The Monsoon-Hadley index (MHI), which is based on the anomalous meridional wind shear, was used as a suitable monthly mean monsoon index to describe the intensity of the South Asian (Indian) summer monsoon circulation [24]:(2)MHI=V850∗-V200∗,where V850∗ and V200∗ are the regional and temporal mean meridional wind anomalies, at 850 hPa and 200 hPa, respectively, over the monsoon region (10°N–30°N, 70°E–110°E) during April–August.


## 2.4. Empirical Orthogonal Function (EOF) Analysis

EOF analysis decomposes the space-time field into a set of orthogonal spatial patterns along with a set of associated, uncorrelated, time indices or principal components (PCs) in a linear fashion. The EOF technique aims to find a new set of variables that capture most of the observed variance from the data, through linear combinations of the original variables, or reduce the large number of variables of the original data to a few variables. It has proven to be a powerful tool for identifying dominant modes of climate variability and tracer analysis [25]. In this study, EOF analysis was applied to the monthly mean TOVMR dataset over East Asia (80°E–140°E, 10°N–50°N) from March 1996 to June 2003 to retrieve the dominant spatiotemporal modes of tropospheric ozone over East Asia.


## 3. The Seasonality of Tropospheric Ozone

In winter (Figure1(a)), high values of TCO (>32 DU) were present along a zonal belt around 30°N and there were low values of TCO (<26 DU) over the Tibetan Plateau and northern China. In spring (Figure 1(b)), TCO was enhanced (>47 DU) along a zonal belt around 30–35°N, due to stratosphere–troposphere exchange (STE), which predominantly occurs at this time of the year within this zonal belt [26]. In summer (Figure 1(c)), the belt of enhanced TCO (greater than 50 DU) moved northward to around 40°N. Here, TCO shows the highest values throughout the year. Some studies have attributed this large increase in ozone in summer to its photochemical production, which is enhanced by the presence of anthropogenic pollution, biogenic volatile organic compounds, and NOx [26, 27]. In autumn (Figure 1(d)), the TCO rapidly decreased and the belt of high TCO moved back towards the lower latitudes. GOME data were not available over Northern India and west of the Himalayas due to a lack of downlinking of GOME data to ground stations; thus these areas are shown in white in Figure 1.Figure 1
Monthly mean tropospheric column ozone (TCO) (unit: Dobson unit (DU)) from GOME (Global Ozone Monitoring Experiment) measurements between March 1996 and June 2003. GOME data are unavailable over the white area due to the lack of downlinking of GOME data to ground stations. The dark thick contours are coastline and the edge of Tibetan Plateau.
(a)
Jan.
(b)
Apr.
(c)
Jul.
(d)
Oct.Note that TCO was lower over the Tibetan Plateau than over other regions in the same latitudes in East Asia during the year. This tropospheric ozone anomaly is sufficiently shown to be clearly noticeable even in total ozone column measurements [28]. The anomaly low TCO over the Tibetan Plateau mainly occurs because of both the unique topography of the area and the tropopause height, which together determine the vertical extent of the tropospheric air column. With elevations up to almost the middle troposphere, the Tibetan Plateau (which extends over 27°N–45°N, 70°E–105°E at an average elevation of ~4 km) has a much shorter tropospheric air column over it than that in other regions at the same latitude. Further, the tropopause pressure over the Tibetan Plateau is lower, which means the tropopause is higher (Figure 2) over this region than at similar latitudes elsewhere in East Asia; this is especially true in summer (Figure 2(c)) as a result of the onset of Asian summer monsoon. Therefore, in order to reduce the influence of topography and tropopause height on tropospheric ozone, as detailed in the methods, the TCO was converted to TOVMR by using the tropopause and surface pressure data from NCEP.Figure 2
The same as Figure1, but for zonal deviations of tropopause pressure (unit: hPa).
(a)
Jan.
(b)
Apr.
(c)
Jul.
(d)
Oct.The seasonality of TOVMR (Figure3) is similar to that of TCO (Figure 1), except over the Tibetan Plateau, where TOVMR is higher than in other regions of the same latitude in East Asia. By excluding the effects of topography and tropopause height, TOVMR has certain advantages over TCO in studying the tropospheric ozone over East Asia. So, the spatiotemporal variations of tropospheric ozone over East Asia were investigated using TOVMR and are described in the following.Figure 3
The same as Figure1, but for tropospheric ozone volume mixing ratio (TOVMR, unit: ppbv).
(a)
Jan.
(b)
Apr.
(c)
Jul.
(d)
Oct.


## 4. EOF Analysis of TOVMR

The two dominant spatial modes of monthly mean TOVMR from March 1996 to June 2003 over East Asia (80°E–140°E, 10°N–50°N) retrieved by EOF analysis (EOF1 and EOF2; Figures4(a) and 4(b), resp.), along with their associated time series (PC1 and PC2; Figures 4(c) and 4(d), resp.), together explained ~90% of the spatiotemporal ozone variability in East Asia. This means that the major characteristics of tropospheric ozone were captured by these two modes. Both modes satisfied North’s criteria [29] and have actual physical meaning.Figure 4
Two dominant patterns retrieved from EOF analysis ((a) EOF1, (b) EOF2) of monthly mean TOVMR (color shaded) and their corresponding time series ((c) PC1, (d) PC2; red: positives, blue: negatives) between March 1996 and June 2003. The yellow contours in (a) are total westerly jet occurrence counts based on 6-hourly ERA-interim data, and the thick green lines show the position of maximum occurrence. Summer (June–August) winds at 200 hPa for the same period are shown by vectors in (b). The red star is the location of Beijing and the red dots are locations of Lhasa, Xining, and Pyramid (Nepal); they are four ozonesonde stations. The square in (a) is the area of northern China; the square in (b) is southern Tibetan Plateau and the area to the south of Tibetan Plateau.
(a)
EOF1 (61.5%)
(b)
EOF2 (29.2%)
(c)
PC1
(d)
PC2


### 4.1. The First EOF Mode (EOF1)

The EOF1 (Figure4(a)) explained 61.5% of the variance in ozone variability, with same-sign values over the entire East Asia, suggesting that the main variability in TOVMR over the entire region is very likely dominated by the same mechanism. The PC1 time series suggested that the maxima occur in May-June and the minima in November-December (Figure 4(c)). This indicates that the contribution of photochemical ozone production plays a significant role in modulating the seasonal variation of the averaged ozone concentration in the troposphere. However, the maxima did not occur in July-August when photochemical production was even stronger. We suspect that some dynamical processes must also be responsible for the formation of EOF1. It is noted that there was a belt of high values of EOF1 around 40°N (Figure 4(a)). The latitudinal location of the high-value belt is very close to that of the downward branch of the Brewer-Dobson circulation (BDC) in the midlatitudes, which is regarded to be a dominant avenue for stratosphere-to-troposphere ozone transport [30, 31]. Additionally, as a horizontal barrier which weakens the north-south exchange, the subtropical westerly jet further maintains the ozone-rich air, brought by the downward transport of the BDC, around 40°N. In the following sections, the correlations between the PC1 time series and the seasonal variation of BDC and westerly jet are analyzed.


#### 4.1.1. The Correlation between EOF1 and BDC Intensity

The BDC is the meridional transport circulation system, which implies upward motion of air in the tropics and downward motion in the subtropics. Dobson [32] successfully explained the meridional distribution of ozone and water vapor by using the BDC, which is mainly driven by stratospheric planetary waves. As a representation of the planetary wave forcing, the vertical component of the Eliassen-Palm- (EP-) flux (EP-Fz) drives the BDC and further affects the meridional transport of ozone [33]. In the following text, we describe how we used the EP-Fz to study the relationship between the BDC and ozone variability in the region that had high levels of TOVMR in the EOF1 mode.The three-dimensional EP-flux [34] was calculated based on the monthly mean ERA-interim zonal wind and temperature data. The mean EP-Fz within the region of high TOVMR values in EOF1 mode (100 hPa, 80–140°E, 35–45°N) was used to characterize the ozone transport from the stratosphere to the troposphere by the BDC. The EP-Fz was high in winter and low in summer (Figure 5(a)), suggesting that the BDC transports more ozone-rich air from lower latitudes to the higher latitudes in stratosphere in winter. However, the maximal tropospheric ozone occurred 5−7 months after the EP-Fz maximum, indicating that once stratospheric ozone has been transported from tropics to midlatitudes by the BDC, it takes several months to be transported through the tropopause and into the troposphere in the subtropics [30]. The lagged correlations between the EP-Fz and GOME tropospheric ozone (Figure 5(b)) indicate that the maximal tropospheric ozone seen in PC1 occurred five months after the EP-Fz maximum (r=0.9), and the maximal GOME ozone (without EOF analysis) occurred six months after the EP-Fz maximum (r=0.88). Based on the ozonesonde measurements over Beijing, which is located in the region of high TOVMR values in EOF1 mode, the maximal tropospheric ozone over Beijing occurred six months after the EP-Fz maximum (r=0.74). The lagged correlations between the EP-Fz and tropospheric ozone (both satellite and ozonesonde) were significant at the 95% confidence level, suggesting that the BDC does play an important role in the formation of the tropospheric ozone pattern seen in EOF1.Figure 5
(a) Time series of the regional mean (80°E–140°E; 35°N–45°N) vertical EP-flux at 100 hPa between January 1996 and December 2010, PC1 decomposed from GOME TOVMR (PC1-O3) and GOME TOVMR (GOME-O3) between March 1996 and June 2003 over northern China, and ozonesonde observed tropospheric ozone mixing ratio (Sonde-O3) over Beijing from September 2002 to December 2010. (b) Lag correlation coefficients between EP-flux and the time series of ozone (red: PC1-O3 over northern China; green: GOME ozone over northern China; blue: ozonesonde over Beijing).
(a)
(b)


#### 4.1.2. The Correlation between EOF1 and the Subtropical Westerly Jet

According to previous studies [35–37], the subtropical westerly jet can block the horizontal ozone exchange between high and low latitudes. Separated by high topography, the two maxima of the subtropical westerly jet occurrence (green lines in Figure 4(a)) exist on the northern and southern edges of the Tibetan Plateau. However, the high values of TOVMR in the EOF1 pattern only existed on the northern edge of the Tibetan Plateau; here, the ozone-rich air brought by the downward transport of the BDC from the stratosphere is blocked by the subtropical westerly jet and accumulates north of the jet.As a result of BDC transportation and blocking effort of subtropical westerly jet, the high ozone produced by photochemical peaked in May-June. Although photochemical production was even stronger in the later July-August, the weakening of BDC transportation and the strength of subtropical westerly jet led to the decrease in ozone during this period.


### 4.2. The Second EOF Mode (EOF2)

The EOF2 mode explained 29.2% of the variance, with an opposite-sign pattern on either side of 35°N (Figure4(b)). The high values of TOVMR seen in EOF2 were mainly located to the south of the Tibetan Plateau and in the Bay of Bengal. The positive maxima of PC2 (Figure 4(d)) occurred in spring (April-May), and the negative minima occurred in summer (July-August). So, it can be concluded that tropospheric ozone, over the areas to the south of the Tibetan Plateau and in the Bay of Bengal, is higher in spring and lower in summer.The PC2 changed rapidly from positive to negative in May-June, indicating that the tropospheric ozone over the area to the south of the Tibetan Plateau and in the Bay of Bengal decreased dramatically during this period. Since this region is located within the area of the summer monsoon anticyclone, which begins during May-June, the Asian summer monsoon could be the main reason for the observed EOF2 mode.There were similar trends (r=0.97) between the PC2 pattern and surface observations from Pyramid, Nepal (5079 m a.s.l.; located on the southern edge of the Tibetan Plateau) (Figure 6). Because PC2 describes tropospheric ozone and the Pyramid observations only recorded surface ozone concentrations, PC2 was generally higher than the ozone observations from Pyramid, except in June, when they were almost equal. This equality can be attributed to the onset of the Asian summer monsoon, which transports air containing less ozone into the region in June; as a result, the tropospheric ozone is reduced and becomes almost equivalent to the surface ozone.Figure 6
Seasonality of surface ozone at Pyramid station (Pyramid-O3) from March 2006 to December 2010 and the regional mean (within ±1°, centered at Pyramid station) PC2 decomposed from GOME TOVMR (PC2-O3) between March 1996 and June 2003. Error bars are standard deviations (±σ).A minimum ozone concentration has been shown to occur in the middle troposphere over the Tibetan Plateau in June, simultaneous with the onset of the Asian summer monsoon [38]. It was suggested that the monsoon anticyclone causes air containing less ozone to be transported from the lower to middle and higher troposphere, by strong upward movements over the Bay of Bengal, driving the air to the Tibetan Plateau. The tropospheric ozone over Pyramid rapidly decreased to be almost equal to surface observations during this process (Figure 6). Blocked by the westerly jet on the northern side of the Tibetan Plateau, the ozone accumulates over the southeast of the Plateau. The existence of this ozone minimum in the middle troposphere over the Tibetan Plateau is consistent with the ozone minimum over Pyramid, resulting from the onset of the Asian summer monsoon.The PC2 over the Tibetan Plateau and to the south of the Tibetan Plateau and the surface ozone observations from Pyramid appear closely related to the South Asian summer monsoon (Figures7(a)–7(c), resp.). However, the relationships between the monsoon and ozone at each location were not simply linear. During March–May, the enhanced photochemistry and ozone exchange between the stratosphere and troposphere over the Tibetan Plateau increased the tropospheric ozone. With the onset of the Asian summer monsoon, during the months May-June, the tropospheric ozone levels over the Tibetan Plateau and to the south of the Tibetan Plateau dramatically decreased, as explained above. Further, the increase in precipitation, due to enhanced convection during the summer monsoon, also played a role in the decrease in ozone.Figure 7
Correlation between the Indian Monsoon index and PC2-O3 over (a) the Tibetan Plateau and (b) south of the Tibetan Plateau between March 1996 and June 2003, and (c) the correlation between the Indian Monsoon index and surface observations of ozone from Pyramid between March 2006 and December 2010.
(a)
TP
(b)
TP-south
(c)
Pyramid-O3


## 4.1. The First EOF Mode (EOF1)

The EOF1 (Figure4(a)) explained 61.5% of the variance in ozone variability, with same-sign values over the entire East Asia, suggesting that the main variability in TOVMR over the entire region is very likely dominated by the same mechanism. The PC1 time series suggested that the maxima occur in May-June and the minima in November-December (Figure 4(c)). This indicates that the contribution of photochemical ozone production plays a significant role in modulating the seasonal variation of the averaged ozone concentration in the troposphere. However, the maxima did not occur in July-August when photochemical production was even stronger. We suspect that some dynamical processes must also be responsible for the formation of EOF1. It is noted that there was a belt of high values of EOF1 around 40°N (Figure 4(a)). The latitudinal location of the high-value belt is very close to that of the downward branch of the Brewer-Dobson circulation (BDC) in the midlatitudes, which is regarded to be a dominant avenue for stratosphere-to-troposphere ozone transport [30, 31]. Additionally, as a horizontal barrier which weakens the north-south exchange, the subtropical westerly jet further maintains the ozone-rich air, brought by the downward transport of the BDC, around 40°N. In the following sections, the correlations between the PC1 time series and the seasonal variation of BDC and westerly jet are analyzed.


### 4.1.1. The Correlation between EOF1 and BDC Intensity

The BDC is the meridional transport circulation system, which implies upward motion of air in the tropics and downward motion in the subtropics. Dobson [32] successfully explained the meridional distribution of ozone and water vapor by using the BDC, which is mainly driven by stratospheric planetary waves. As a representation of the planetary wave forcing, the vertical component of the Eliassen-Palm- (EP-) flux (EP-Fz) drives the BDC and further affects the meridional transport of ozone [33]. In the following text, we describe how we used the EP-Fz to study the relationship between the BDC and ozone variability in the region that had high levels of TOVMR in the EOF1 mode.The three-dimensional EP-flux [34] was calculated based on the monthly mean ERA-interim zonal wind and temperature data. The mean EP-Fz within the region of high TOVMR values in EOF1 mode (100 hPa, 80–140°E, 35–45°N) was used to characterize the ozone transport from the stratosphere to the troposphere by the BDC. The EP-Fz was high in winter and low in summer (Figure 5(a)), suggesting that the BDC transports more ozone-rich air from lower latitudes to the higher latitudes in stratosphere in winter. However, the maximal tropospheric ozone occurred 5−7 months after the EP-Fz maximum, indicating that once stratospheric ozone has been transported from tropics to midlatitudes by the BDC, it takes several months to be transported through the tropopause and into the troposphere in the subtropics [30]. The lagged correlations between the EP-Fz and GOME tropospheric ozone (Figure 5(b)) indicate that the maximal tropospheric ozone seen in PC1 occurred five months after the EP-Fz maximum (r=0.9), and the maximal GOME ozone (without EOF analysis) occurred six months after the EP-Fz maximum (r=0.88). Based on the ozonesonde measurements over Beijing, which is located in the region of high TOVMR values in EOF1 mode, the maximal tropospheric ozone over Beijing occurred six months after the EP-Fz maximum (r=0.74). The lagged correlations between the EP-Fz and tropospheric ozone (both satellite and ozonesonde) were significant at the 95% confidence level, suggesting that the BDC does play an important role in the formation of the tropospheric ozone pattern seen in EOF1.Figure 5
(a) Time series of the regional mean (80°E–140°E; 35°N–45°N) vertical EP-flux at 100 hPa between January 1996 and December 2010, PC1 decomposed from GOME TOVMR (PC1-O3) and GOME TOVMR (GOME-O3) between March 1996 and June 2003 over northern China, and ozonesonde observed tropospheric ozone mixing ratio (Sonde-O3) over Beijing from September 2002 to December 2010. (b) Lag correlation coefficients between EP-flux and the time series of ozone (red: PC1-O3 over northern China; green: GOME ozone over northern China; blue: ozonesonde over Beijing).
(a)
(b)


### 4.1.2. The Correlation between EOF1 and the Subtropical Westerly Jet

According to previous studies [35–37], the subtropical westerly jet can block the horizontal ozone exchange between high and low latitudes. Separated by high topography, the two maxima of the subtropical westerly jet occurrence (green lines in Figure 4(a)) exist on the northern and southern edges of the Tibetan Plateau. However, the high values of TOVMR in the EOF1 pattern only existed on the northern edge of the Tibetan Plateau; here, the ozone-rich air brought by the downward transport of the BDC from the stratosphere is blocked by the subtropical westerly jet and accumulates north of the jet.As a result of BDC transportation and blocking effort of subtropical westerly jet, the high ozone produced by photochemical peaked in May-June. Although photochemical production was even stronger in the later July-August, the weakening of BDC transportation and the strength of subtropical westerly jet led to the decrease in ozone during this period.


## 4.1.1. The Correlation between EOF1 and BDC Intensity

The BDC is the meridional transport circulation system, which implies upward motion of air in the tropics and downward motion in the subtropics. Dobson [32] successfully explained the meridional distribution of ozone and water vapor by using the BDC, which is mainly driven by stratospheric planetary waves. As a representation of the planetary wave forcing, the vertical component of the Eliassen-Palm- (EP-) flux (EP-Fz) drives the BDC and further affects the meridional transport of ozone [33]. In the following text, we describe how we used the EP-Fz to study the relationship between the BDC and ozone variability in the region that had high levels of TOVMR in the EOF1 mode.The three-dimensional EP-flux [34] was calculated based on the monthly mean ERA-interim zonal wind and temperature data. The mean EP-Fz within the region of high TOVMR values in EOF1 mode (100 hPa, 80–140°E, 35–45°N) was used to characterize the ozone transport from the stratosphere to the troposphere by the BDC. The EP-Fz was high in winter and low in summer (Figure 5(a)), suggesting that the BDC transports more ozone-rich air from lower latitudes to the higher latitudes in stratosphere in winter. However, the maximal tropospheric ozone occurred 5−7 months after the EP-Fz maximum, indicating that once stratospheric ozone has been transported from tropics to midlatitudes by the BDC, it takes several months to be transported through the tropopause and into the troposphere in the subtropics [30]. The lagged correlations between the EP-Fz and GOME tropospheric ozone (Figure 5(b)) indicate that the maximal tropospheric ozone seen in PC1 occurred five months after the EP-Fz maximum (r=0.9), and the maximal GOME ozone (without EOF analysis) occurred six months after the EP-Fz maximum (r=0.88). Based on the ozonesonde measurements over Beijing, which is located in the region of high TOVMR values in EOF1 mode, the maximal tropospheric ozone over Beijing occurred six months after the EP-Fz maximum (r=0.74). The lagged correlations between the EP-Fz and tropospheric ozone (both satellite and ozonesonde) were significant at the 95% confidence level, suggesting that the BDC does play an important role in the formation of the tropospheric ozone pattern seen in EOF1.Figure 5
(a) Time series of the regional mean (80°E–140°E; 35°N–45°N) vertical EP-flux at 100 hPa between January 1996 and December 2010, PC1 decomposed from GOME TOVMR (PC1-O3) and GOME TOVMR (GOME-O3) between March 1996 and June 2003 over northern China, and ozonesonde observed tropospheric ozone mixing ratio (Sonde-O3) over Beijing from September 2002 to December 2010. (b) Lag correlation coefficients between EP-flux and the time series of ozone (red: PC1-O3 over northern China; green: GOME ozone over northern China; blue: ozonesonde over Beijing).
(a)
(b)


## 4.1.2. The Correlation between EOF1 and the Subtropical Westerly Jet

According to previous studies [35–37], the subtropical westerly jet can block the horizontal ozone exchange between high and low latitudes. Separated by high topography, the two maxima of the subtropical westerly jet occurrence (green lines in Figure 4(a)) exist on the northern and southern edges of the Tibetan Plateau. However, the high values of TOVMR in the EOF1 pattern only existed on the northern edge of the Tibetan Plateau; here, the ozone-rich air brought by the downward transport of the BDC from the stratosphere is blocked by the subtropical westerly jet and accumulates north of the jet.As a result of BDC transportation and blocking effort of subtropical westerly jet, the high ozone produced by photochemical peaked in May-June. Although photochemical production was even stronger in the later July-August, the weakening of BDC transportation and the strength of subtropical westerly jet led to the decrease in ozone during this period.


## 4.2. The Second EOF Mode (EOF2)

The EOF2 mode explained 29.2% of the variance, with an opposite-sign pattern on either side of 35°N (Figure4(b)). The high values of TOVMR seen in EOF2 were mainly located to the south of the Tibetan Plateau and in the Bay of Bengal. The positive maxima of PC2 (Figure 4(d)) occurred in spring (April-May), and the negative minima occurred in summer (July-August). So, it can be concluded that tropospheric ozone, over the areas to the south of the Tibetan Plateau and in the Bay of Bengal, is higher in spring and lower in summer.The PC2 changed rapidly from positive to negative in May-June, indicating that the tropospheric ozone over the area to the south of the Tibetan Plateau and in the Bay of Bengal decreased dramatically during this period. Since this region is located within the area of the summer monsoon anticyclone, which begins during May-June, the Asian summer monsoon could be the main reason for the observed EOF2 mode.There were similar trends (r=0.97) between the PC2 pattern and surface observations from Pyramid, Nepal (5079 m a.s.l.; located on the southern edge of the Tibetan Plateau) (Figure 6). Because PC2 describes tropospheric ozone and the Pyramid observations only recorded surface ozone concentrations, PC2 was generally higher than the ozone observations from Pyramid, except in June, when they were almost equal. This equality can be attributed to the onset of the Asian summer monsoon, which transports air containing less ozone into the region in June; as a result, the tropospheric ozone is reduced and becomes almost equivalent to the surface ozone.Figure 6
Seasonality of surface ozone at Pyramid station (Pyramid-O3) from March 2006 to December 2010 and the regional mean (within ±1°, centered at Pyramid station) PC2 decomposed from GOME TOVMR (PC2-O3) between March 1996 and June 2003. Error bars are standard deviations (±σ).A minimum ozone concentration has been shown to occur in the middle troposphere over the Tibetan Plateau in June, simultaneous with the onset of the Asian summer monsoon [38]. It was suggested that the monsoon anticyclone causes air containing less ozone to be transported from the lower to middle and higher troposphere, by strong upward movements over the Bay of Bengal, driving the air to the Tibetan Plateau. The tropospheric ozone over Pyramid rapidly decreased to be almost equal to surface observations during this process (Figure 6). Blocked by the westerly jet on the northern side of the Tibetan Plateau, the ozone accumulates over the southeast of the Plateau. The existence of this ozone minimum in the middle troposphere over the Tibetan Plateau is consistent with the ozone minimum over Pyramid, resulting from the onset of the Asian summer monsoon.The PC2 over the Tibetan Plateau and to the south of the Tibetan Plateau and the surface ozone observations from Pyramid appear closely related to the South Asian summer monsoon (Figures7(a)–7(c), resp.). However, the relationships between the monsoon and ozone at each location were not simply linear. During March–May, the enhanced photochemistry and ozone exchange between the stratosphere and troposphere over the Tibetan Plateau increased the tropospheric ozone. With the onset of the Asian summer monsoon, during the months May-June, the tropospheric ozone levels over the Tibetan Plateau and to the south of the Tibetan Plateau dramatically decreased, as explained above. Further, the increase in precipitation, due to enhanced convection during the summer monsoon, also played a role in the decrease in ozone.Figure 7
Correlation between the Indian Monsoon index and PC2-O3 over (a) the Tibetan Plateau and (b) south of the Tibetan Plateau between March 1996 and June 2003, and (c) the correlation between the Indian Monsoon index and surface observations of ozone from Pyramid between March 2006 and December 2010.
(a)
TP
(b)
TP-south
(c)
Pyramid-O3


## 5. Conclusions

The spatiotemporal characteristics of tropospheric ozone over East Asia were analyzed using tropospheric ozone data from the GOME satellite and meteorological datasets from the ERA-interim reanalysis dataset. Generally, the TCO was the lowest in winter and the highest in summer, with a TCO minimum present over the Tibetan Plateau. There was a belt of high TCO, which occurred at 30°N in winter and moved northward to 40°N in summer. To reduce the influence of topography and the tropopause height on TCO, we calculated the average ozone concentration in the troposphere (TOVMR). The seasonality of TOVMR was similar to that of TCO, except that the TOVMR over the Tibetan Plateau was the highest in East Asia throughout the year.EOF analysis was applied to characterize the spatiotemporal variations in TOVMR. The two dominant spatial patterns (EOF1 and EOF2) explained ~90% of the total variance in TOVMR. The EOF1 mode, which explained 61.5% of the total variance, showed a same-sign distribution over all of East Asia, with a belt of enhanced ozone concentrations around 40°N. The PC1 time series showed that the averaged ozone concentration in the troposphere was higher in summer and lower in winter, indicating the contribution of photochemical ozone production. Further analysis suggested that the high-value belt of ozone concentrations around 40°N was highly related to the vertical transport of ozone-rich air from the stratosphere to the troposphere by the downward branch of the BDC. This ozone-rich air is then blocked by the subtropical westerly jet and accumulates to the north of the jet.The EOF2 mode explained 29.2% of the total variance, with an opposite-sign pattern on the northern and southern sides of 35°N. The high values of TOVMR in EOF2 were located to the south of the Tibetan Plateau and in the Bay of Bengal. Tropospheric ozone over this region decreased dramatically in May-June, when the anticyclonic circulation transports ozone-poor air from the upwelling area over the Bay of Bengal towards the Tibetan Plateau during the onset of the Asian summer monsoon. The high correlations between the Monsoon-Hadley index (MHI) and ozone over three locations in this region confirmed the dominant contribution of the Asian summer monsoon to the EOF2 mode.To quantify the relative contributions of photochemistry and transport to the tropospheric ozone budget and its seasonal variation shown in EOF1, a numerical study based on the chemistry transport models should be performed in the future.



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*Source: 879578-2015-09-13.xml*