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Intraseasonal Variations of the Tropical Total Ozone and
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Their Connection to the Madden-Julian Oscillation
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Baijun Tian
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Jet Propulsion Laboratory, California Institute of Technology, Pasadena, CA
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Yuk L. Yung
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Div of Geological and Planetary Sciences, California Institute of Technology, Pasadena, CA.
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Duane E. Waliser
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Jet Propulsion Laboratory, California Institute of Technology, Pasadena, CA
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Tomasz Tyranowski
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Jagiellonian University, Krakow, Poland
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Le Kuai
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Div of Geological and Planetary Sciences, California Institute of Technology, Pasadena, CA.
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Fredrick W. Irion
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Jet Propulsion Laboratory, California Institute of Technology, Pasadena, CA
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J. Geophys. Res.
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Drafted – 10/08/2006
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Corresponding author address: Dr. Baijun Tian, Jet Propulsion Laboratory, California Institute of
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Technology, M/S 183-501, 4800 Oak Grove Dr., Pasadena CA 91109. Email: Baijun.Tian@jpl.nasa.gov.
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Abstract
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The total ozone from the Total Ozone Mapping Spectrometer (TOMS) instrument on the
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Nimbus 7 spacecraft and the Atmospheric Infrared Sounder (AIRS) instrument on the Aqua
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spacecraft, the rainfall from the Global Precipitation Climatology Project (GPCP), and the
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dynamic fields (geopotential height and stream function) from the NCEP/NCAR reanalysis are
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employed to study the intraseasonal (30–90 day) variations of the tropical total ozone and their
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connection to the Madden-Julian Oscillation (MJO). We found that the intraseasonal variations
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of the tropical total ozone are large (around 5 DU) in both AIRS and TOMS and comparable to
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those associated with annual cycle, quasi-biennial oscillation, El Nino and Southern Oscillation,
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and solar cycle. In particular, the intraseasonal total ozone anomalies are mainly evident over the
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subtropics, with a systematic relationship with the equatorial MJO convection anomaly
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throughout the MJO cycle. Positive subtropical total ozone anomalies are typically collocated
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with or lie to the west of the equatorial suppressed MJO convection and negative subtropical
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total ozone anomalies are typically collocated with or lie to the west of the equatorial enhanced
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MJO convection. The subtropical total ozone anomalies propagate eastward at a phase speed of
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~5 m s-1 similar to the equatorial MJO convection anomaly in the Eastern Hemisphere and they
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propagate much faster (~15 m s-1) in the Western Hemisphere when the equatorial MJO
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convection anomaly disappears. Comparison of the horizontal maps of the TOMS total ozone
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anomalies and the NCEP 200-hPa geopotential height and stream function anomalies show that
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negative (positive) subtropical total ozone anomalies are collocated with the subtropical upper-
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tropospheric anticyclones (cyclones) and positive (negative) geopotential height anomalies with
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a high negative correlation (~–0.75) between the total ozone and geopotential height anomalies.
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This indicates that the subtropical total ozone anomalies are mainly dynamically driven as a
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result of the subtropical upper-tropospheric cyclones or anticyclones generated by the equatorial
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MJO convection. AIRS also indicates that negative (positive) equatorial total ozone anomalies
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are collocated with the enhanced (suppressed) equatorial MJO convection, while TOMS does
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not.
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1. Introduction
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The total column abundance of the ozone in the tropical atmosphere represents an
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intricate interaction between chemical and dynamical processes [Brasseur et al., 1999]. Thus, the
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tropical total ozone and its variability have been extensively studied especially after the launch of
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the Total Ozone Mapping Spectrometer (TOMS) instrument on the Nimbus 7 spacecraft
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[Krueger 1989]. Previous studies have investigated the trend [Stolarski, 1986; 1992; Herman et
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al., 1991], annual cycle [Shiotani, 1992], quasi-biennial oscillation (QBO) [Oltmans and London,
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1982; Bowman, 1989; Zawodny and McCormick, 1991; Shiotani, 1992; Tung and Yang, 1994a;
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1994b], El Niño-Southern Oscillation (ENSO) or interannual variation [Shiotani, 1992; Randel
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and Cobb, 1994; Kayano, 1997; Camp et al., 2003], and solar cycle [Hood, 1997] of the tropical
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total ozone. It was found that the tropical total ozone varies on the order of ±10 Dobson Unit
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(DU) (~3% of the mean) for annual cycle and ENSO, about ±15 DU (~5% of the mean) for
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QBO, and about ±5 DU (~2% of the mean) for solar cycle. However, very few studies have
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investigated the intraseasonal (30–90 day) variations of the tropical total ozone. The study by
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Gao and Stanford [1990] indicated that there is a possible intraseasonal variability in the tropical
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total ozone. However, the spatial and temporal patterns of the intraseasonal variations of the
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tropical total ozone have not been well documented. In particular, the physical and dynamical
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processes that are responsible for the intraseasonal variations of the tropical total ozone have
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never been investigated.
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The Madden-Julian Oscillation (MJO; aka Intraseasonal Oscillation) [Madden and Julian,
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1972] is the dominant component of the intraseasonal variability in the tropical atmosphere.
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Since its discovery, the MJO has continued to be a topic of significant interest due to its
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extensive interactions with other components of the climate system and the fact that it represents
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a connection between the better understood weather and seasonal-to-interannual climate
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variations. The MJO is characterized by eastward-propagating, large-scale baroclinic oscillations
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in the tropical wind field [Madden and Julian, 1972; Madden and Julian, 1994]. Over the
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warmest tropical waters, in the equatorial Indian and western Pacific Oceans, the disturbance
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manifests itself in the form of large-scale convection anomalies which interact with the upper-
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level atmospheric flow, surface winds and heat fluxes [Knutson and Weickmann, 1987; Rui and
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Wang, 1990; Hendon and Salby, 1994; Matthews et al., 2004]. In these regions, where the
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convective activity is strong, the oscillation propagates slowly (~5 m s-1) and the interaction with
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the extra-tropics is greatest. Once the disturbance reaches the date line, and thus cooler equatorial
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waters, convection subsides and the remaining dynamical disturbance behaves much like a
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damped Kelvin wave with a faster propagation speed [~15 m s-1, Hendon and Salby, 1994]. The
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above characteristics tend to be most strongly exhibited during the boreal winter and spring
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(November-April) when the Indo-Pacific warm pool is centered near the equator. During the
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boreal summer and fall (May-October), the change in the large-scale circulation associated with
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the Asian summer monsoon results in the largest-scale aspects of the disturbances propagating
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more northeastward, from the equatorial Indian Ocean into Southeast Asia [e.g., Wang and Rui,
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1990; Waliser, 2006]. For more comprehensive reviews of the MJO and related issues, the reader
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is referred to Madden and Julian [1994], Lau and Waliser [2005], and Zhang [2005]. From the
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discussion above, we can see that the large-scale MJO convection and circulation anomalies have
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been well documented and understood; however, their connection to the intraseasonal variations
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of the tropical total ozone has never been investigated.
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The purpose of this study is to investigate the intraseasonal variations of the tropical total
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ozone and its possible connection to the large-scale MJO convection and circulation anomalies.
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We are attempting to address the following three questions. 1) Are there any intraseasonal
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variations of the tropical total ozone? 2) If yes, how large are these variations and what the
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spatial and temporal patterns of these variations are? 3) What physical or dynamical processes
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are responsible for these variations? Is there any connection between the large-scale MJO
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convection and circulation anomalies and the intraseasonal variations of the total ozone?
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The outline for the rest of this paper is as follows: The data and methodology are
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introduced in section 2. Section 3 presents the main results of this study and its interpretation.
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Section 5 provides a summary of the major findings of this study.
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2. Data and Methodology
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For this study, we have used two data sets for the tropical total ozone: The Atmospheric
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Infrared Sounder (AIRS) on the Aqua satellite and the TOMS on the Nimbus 7 satellite. The
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AIRS, together with Advanced Microwave Sounding Unit, form the integrated hyperspectral
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infrared and microwave atmospheric sounding system which has been operational since
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September 2002 [Chahine et al., 2006]. The primary AIRS products are twice daily global fields
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of atmospheric temperature and humidity profiles, ozone profile, surface skin temperature, and
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cloud related parameters [Susskind et al., 2006]. In this study, we use AIRS Level 3 Version 4
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total ozone product on a 1º × 1º latitude-longitude grid from September 2002 to July 2006. The
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AIRS ozone retrieval is a research product that is currently undergoing validation. Gettelman et
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al. [2004] have compared AIRS ozone retrieval with research aircraft measurements in the upper
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troposphere; their limited comparisons suggest that the AIRS ozone has a 30% positive bias in
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the upper troposphere but can reasonably track variability over a range of mixing ratios from
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approximately 50–500 ppbv.
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The Nimbus 7 TOMS provided daily global coverage of the Earth’s total ozone from 24
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October 1978 to 6 May 1993 by measuring backscattered ultraviolet (UV) sunlight [Krueger
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1989; McPeters et al., 1996]. The TOMS ozone data have been well validated and extensively
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used for climate studies (see introduction). The TOMS will also provide more confidence on
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MJO results because its longer record (13 years) allows more samples of MJO events than AIRS
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(4 years). The TOMS data are on a 3º × 5º grid averaged from their original 1º × 1.25º grid. Only
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data from 1 January 1980 to 31 December 1992 were used in this study.
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To identify MJO events, the global pentad rainfall data from the Global Precipitation
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Climatology Project (GPCP, Xie et al. 2003) covering from 1 January 1979 to June 30 2006
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(should update to June 2006) and on a 2.5º by 2.5º grid were used. In the following discussion,
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rainfall is used as a proxy for MJO convection. To identify the MJO dynamical fields, daily
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geopotential height and stream function from the National Center for Environmental
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Prediction/National Center for Atmospheric Research reanalysis [NCEP, Kalnay et al. 1996]
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covering from 1979 to 2002 (up to July 2006??) were used. The spatial resolution of the NCEP
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reanalysis is 2.5° x 2.5°.
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The MJO analysis and composite procedure of Tian et al. [2006] were followed for this
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study. All the data were first binned into 5-day average (i.e. pentad) values. Intraseasonal
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anomalies were obtained by removing the annual cycle and then band-pass filtering (30–90 day)
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the data. To isolate the dominant structure of the MJO, an extended empirical orthogonal
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function (EEOF) was applied using time lags of ±5 pentads on boreal winter rainfall for the
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region 30ºS-30ºN and 30ºE-150ºW. Next, MJO events were chosen based on the amplitude
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pentad time series of the first EEOF mode of rainfall anomaly. Figure 1 shows the dates of the
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selected MJO events for TOMS (a) and AIRS (b) data based on the rainfall anomaly. 24 MJO
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events were selected for TOMS and 8 MJO events for AIRS. For each selected MJO event, the
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corresponding 11-pentad rainfall, total ozone, geopotential height, and stream function anomalies
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were extracted for each data set (GPCP, AIRS, TOMS, and NCEP). A composite MJO cycle (11
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pentads) of the anomalies was then obtained by averaging the selected MJO events.
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3. Results and Discussions
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3.1 Intraseasonal variations of the tropical total ozone
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Figure 2 shows the horizontal maps of the TOMS total ozone MJO anomalies (DU, color
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shading) for the composite MJO cycle. For simplicity, only lags ±4, ±2, and 0 pentads of the
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MJO cycle are shown. In addition, the contour plots overlaid on the color shadings are the
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corresponding MJO-related GPCP rainfall anomalies (mm day-1). Note that the magnitude of the
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composite ozone anomalies ranges up to about ±2.5 DU. However, inspection of the individual
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events shows that they range up to about ±5 DU (~2% of the mean) but the compositing
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procedure reduces the signal amplitude. This indicates that the intraseasonal variations of the
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tropical total ozone are significant and comparable to those associated with other times scales,
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such as the annual cycle, QBO, ENSO, and solar cycle. (Confidence limit)
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Over the equatorial regions (10ºS–10ºN), the total ozone variations are rather small (<1
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DU). On the other hand, significant total ozone intraseasonal variations (~2.5 DU) are mainly
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found over the subtropical regions, with maxima near 25º latitudes, with great symmetry between
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the Southern and Northern Hemispheres. In particular, systematic relationship is persistent
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throughout the MJO cycle between the subtropical total ozone anomalies and the equatorial MJO
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convection anomalies in the Eastern Hemisphere, where MJO convection is active. The negative
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subtropical total ozone anomalies are typically collocated with or lie to the west of the enhanced
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equatorial MJO convection and the positive subtropical total ozone anomalies are generally
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collocated with or lie to the west of the suppressed equatorial MJO convection. The subtropical
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total ozone anomalies propagate eastward at a phase speed of ~5 m s-1 similar to the equatorial
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MJO convection anomaly. In the Western Hemisphere where the equatorial MJO convection
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anomaly subsides, the remaining subtropical total ozone anomalies are still large and propagate
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eastward at a much faster phase speed ~15 m s-1.
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Diagram similar to Figure 2 but for the AIRS total ozone anomalies is presented in Figure
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3. The total ozone anomalies in AIRS are much larger and noisier than TOMS. This is due
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probably to the fact that much fewer MJO events considered in AIRS than TOMS. Comparison
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of Figures 2 and 3 indicates both striking similarity and significant difference exist in the total
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ozone anomalies between TOMS and AIRS. The similarity is mainly over the subtropics, while
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the difference is at the equatorial region. Over the subtropics, TOMS and AIRS are consistent
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with each other because both TOMS and AIRS show large total ozone anomalies (~2 DU) over
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the subtropics although the total ozone anomalies are much noisier in AIRS than TOMS. Similar
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to TOMS, AIRS also indicates similar systematic relationship between the subtropical total
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ozone anomalies and the equatorial MJO convection anomalies comparing to TOMS: negative
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(positive) subtropical total ozone anomalies are collocated with or lie to the west of the enhanced
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(suppressed) equatorial MJO convection. The subtropical total ozone anomalies in AIRS also
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propagate eastward at a phase speed of ~5 m s-1 in the Western Hemisphere and much faster (~15
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m s-1) in the Western Hemisphere. Given the stark different techniques and time periods in
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measuring the total ozone from TOMS (backscattered solar UV radiation, 1980-1992) and AIRS
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(infrared, 2002-2006), the similarity in the subtropical total ozone anomalies and their
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relationship to the equatorial MJO convection anomaly between TOMS and AIRS is striking.
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This indicates that the intraseasonal variations of the subtropical total ozone and their
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relationship with the equatorial MJO convection anomaly should be robust rather than an artifact
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of the instruments. The physical or dynamical processes that are responsible for the intraseasonal
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variations of the subtropical total ozone will be further discussed in subsection 3.2.
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Over the equatorial regions, TOMS shows that the equatorial total ozone anomalies are
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negligible (<1 DU); however, AIRS indicates the equatorial total ozone anomalies are significant
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(~2 DU) especially in the regions where MJO convection is active, such as the Eastern
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Hemisphere and South America. In AIRS, negative equatorial total ozone anomalies are typically
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collocated with the enhanced equatorial MJO convection and positive equatorial total ozone
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anomalies are generally collocated with the suppressed equatorial MJO convection. The
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equatorial total ozone anomalies also propagate eastward at a phase speed of ~5 m s-1 similar to
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the equatorial MJO convection anomaly. The relationship between the equatorial total ozone and
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convection anomalies in the intraseasonal time scale is consistent with that found in the annual
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cycle and ENSO time scales [e.g., Shiotani 1992; Hasebe 1993].
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3.2 Connection to the MJO dynamics
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To understand the physical or dynamical processes that are responsible for the
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intraseasonal total ozone anomalies discussed above, the horizontal maps of the TOMS total
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ozone (DU, color shading) and the NCEP 200-hPa geopotential height (m, black contours) MJO
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anomalies for the composite MJO cycle are presented in Figure 4. Clearly, negative (positive)
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subtropical total ozone anomalies are typically collocated with positive (negative) subtropical
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200-hPa geopotential height anomalies with a high negative correlation (~–0.75) between them.
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(Confidence limit?) Similar analysis based on the geopotential height at 100-hPa also indicates a
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strong negative correlation between the subtropical total ozone and 100-hPa geopotential height
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anomalies. This indicates that the subtropical total ozone anomalies are mainly driven by the
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vertical movement of the tropopause layer and its height. It is well known that concentrations of
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ozone are much higher in the stratosphere and much lower in the troposphere with a sharp
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boundary at tropopause [e.g., Fujiwara et al., 1998; Steinbrecht et al. 1998; Pan et al., 2004; more
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refs?]. Thus, any process that depresses the height of the tropopause will tend to replace ozone-
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poor tropospheric air by ozone-rich stratospheric air, and the total ozone will increase. On the
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other hand, any process that lifts the tropopause height will tend to replace ozone-rich
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stratospheric air by ozone-poor tropospheric air, and the total ozone will decrease. This
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relationship has been noted at many time scales and by many researchers, for example, Dobson
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et al. [1929; 1946], Reed [1950], Schubert and Munteanu [1988], Krueger [1989], Mote et al.
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[1991], Salby and Callaghan [1993], and Steinbrecht et al. [1998]. Our results on the relationship
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between the subtropical total ozone and the subtropical upper-tropospheric geopotential height
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anomalies in the intraseasonal time scale are consistent with these previous studies.
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To further elucidate the dynamical processes that cause the vertical movement of the
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tropopause layer that are responsible for the intraseasonal total ozone anomalies, the horizontal
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maps of the NCEP 200-hPa stream function (106 m2 s-1, color shading) and geopotential height
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(m, black contours) MJO anomalies for the composite MJO cycle are shown in Figure 5. In
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addition, the green contour plots overlaid on the color shadings and black contours are the
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corresponding MJO-related GPCP rainfall anomalies (mm day-1). Please note negative (positive)
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stream functions indicate a cyclone (an anticyclone) in the Northern Hemisphere, while negative
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stream (positive) functions indicate an anticyclone (a cyclone) in the Southern Hemisphere.
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Figure 5 shows that a subtropical upper-tropospheric anticyclonic couplet is collocated with or
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lies to the west of the enhanced equatorial MJO convection and a subtropical upper-tropospheric
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cyclonic couplet is collocated with or lies to the west of the reduced equatorial MJO convection.
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To the east of the enhanced (reduced) equatorial MJO convection are equatorial upper-
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tropospheric westerly (easterly) anomalies. These upper-tropospheric large-scale circulation
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features associated with the equatorial MJO convection have been well documented [e.g.,
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Knutson and Weickmann, 1987; Rui and Wang, 1990; Hendon and Salby, 1994; Matthews et al.,
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2004] and can be interpreted as an equatorial Rossby-Kelvin wave response to the equatorial
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MJO convection [Gill 1980].
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From Figure 5, we can clearly see that negative subtropical upper-tropospheric
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geopotential height anomalies are typically collocated with the subtropical upper-tropospheric
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cyclones and positive subtropical upper-tropospheric geopotential height anomalies are typically
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collocated with the subtropical upper-tropospheric anticyclones, with a high positive correlation
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(~0.92) between geopotential height and stream function anomalies. This indicates that the
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vertical movement of the subtropical tropopause layer is mainly a dynamical result of the upper-
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tropospheric subtropical cyclones or anticyclones.
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Diagram similar to Figure 4 but for the TOMS total ozone and the NCEP 200-hPa stream
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function (not shown) also clearly demonstrate that negative (positive) subtropical total ozone
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anomalies are typically collocated with the subtropical upper-tropospheric anticyclones
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(cyclones), with a high positive correlation (~0.75) between the total ozone and stream function
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anomalies. Combining Figures 2, 4, and 5 together, it is evident that the subtropical total ozone
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anomalies are mainly dynamically driven as a result of the subtropical upper-tropospheric
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cyclones or anticyclones generated by the equatorial MJO convection.
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Over the equatorial regions, the TOMS total ozone and the NCEP 200-hPa geopotential
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height MJO anomalies are both small and their correlation is rather low (~0.15). However, AIRS
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indicates significant equatorial total ozone anomalies are collocated with the equatorial MJO
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convection. Show correlation between the equatorial total ozone anomalies in AIRS and the
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NCEP 200-hPa geopotential height anomalies???? (expect good correlation or not???). This may
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be due to the possible biases in the TOMS total ozone retrieval because TOMS cannot measure
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the tropospheric ozone below optically thick clouds in the tropical deep convective regions
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(Ref???). This indicates that the vertical movement of the tropopause will play a lesser in the
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equatorial total ozone anomalies than in subtropics. There may be a contribution from the
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coupled chemistry and dynamics of ozone in the troposphere and need further investigation.
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4. Conclusions
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This study is the first attempt to document the spatial and temporal patterns of the
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intraseasonal variations of the tropical total ozone and their dynamical connection to the large-
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scale MJO convection and circulation anomalies. This is motivated by the fact that the total
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ozone is an important tracer for atmospheric motions [Dobson et al. 1929; Krueger 1989]. Based
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on the total ozone data from TOMS and AIRS, we found that the intraseasonal variations of the
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tropical total ozone are large (around 5 DU) in both TOMS and AIRS and comparable to those
275
associated with annual cycle, QBO, ENSO, and solar cycle. The intraseasonal total ozone
276
anomalies are mainly evident over the subtropics. In particular, there is a systematic relationship
277
between the subtropical total ozone anomalies and the equatorial MJO convection anomaly, that
278
is, positive anomalies are typically collocated with or lie to the west of the equatorial suppressed
279
MJO convection and negative anomalies are typically collocated with or lie to the west of the
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equatorial enhanced MJO convection. The subtropical total ozone anomalies propagate eastward
281
at a phase speed of ~5 m s-1 similar to the equatorial MJO convection anomaly in the Eastern
13
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Hemisphere and they propagate much faster (~15 m s-1) in the Western Hemisphere when the
283
equatorial MJO convection anomaly disappears. Comparison of the horizontal maps of the
284
TOMS total ozone anomalies and the NCEP 200-hPa geopotential height and stream function
285
anomalies show that negative (positive) subtropical total ozone anomalies are collocated with the
286
subtropical upper-tropospheric anticyclones (cyclones) and positive (negative) geopotential
287
height anomalies with a high negative correlation (~–0.75) between the total ozone and
288
geopotential height anomalies. This indicates that the subtropical total ozone anomalies are
289
mainly dynamically driven as a result of the subtropical upper-tropospheric cyclones or
290
anticyclones generated by the equatorial MJO convection. AIRS also indicates that negative
291
(positive) equatorial total ozone anomalies are collocated with the enhanced (suppressed)
292
equatorial MJO convection, while TOMS does not. Thus, there may be a contribution to the
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equatorial total ozone anomalies from the coupled chemistry and dynamics of ozone in the
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troposphere.
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The strong connection between the total ozone variation and the large-scale MJO
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convection and circulation anomalies has important implications for the future MJO studies. The
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total ozone, unlike winds and geopotential height, has been routinely monitored on a global basis
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by satellite since the launch of TOMS in 1978. Thus, the abundance of the satellite total ozone
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data will provide an excellent tool to study the large-scale MJO convection and circulation
300
anomalies and their impact on the global weather and climate.
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Acknowledgements
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The research described in this paper was carried out at the Jet Propulsion Laboratory
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(JPL), California Institute of Technology, under a contract with NASA. It was jointly supported
14
305
by the Research and Technology Development program, Human Resources Development fund,
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and the Atmospheric Infrared Sounder project at JPL. The AIRS and TOMS ozone data and
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GPCP rainfall data were downloaded from GSFC DAAC, respectively.
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Figure Captions
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Figure 1: The dates of the selected MJO events for TOMS (a) and AIRS periods based on the
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amplitude pentad time series for the first EEOF mode of GPCP (a) and TRMM (b)
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rainfall anomaly from NH wintertime (November–April) and the region 30°N–30°S
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and 30°E–150°W.
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Figure 2: Composite TOMS total ozone MJO anomalies (DU, color shading). The superimposed
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solid (dashed) black contours denote the GPCP rainfall MJO anomalies (mm day-1).
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For simplicity, only lags -4, -2, 0, +2, and +4 pentads of the MJO cycle are shown.
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Figure 3: As Figure 2 but for the AIRS total ozone and TRMM rainfall MJO anomalies.
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Figure 4: Composite MJO cycles of the TOMS total ozone (DU, color shading) and the NCEP
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200-hPa geopotential height (m, black contours) MJO anomalies.
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Figure 5: Composite MJO cycles of the NCEP 200-hPa stream function (106 m2 s-1, color
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shading) and the NCEP 200-hPa geopotential height (m, black contours) MJO
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anomalies.
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Figure 1: The dates of the selected MJO events for TOMS (a) and AIRS periods based on the
amplitude pentad time series for the first EEOF mode of GPCP (a) and TRMM (b) rainfall anomaly
from NH wintertime (November–April) and the region 30°N–30°S and 30°E–150°W.
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Figure 2: Composite TOMS total ozone MJO anomalies (DU, color shading). The
superimposed solid (dashed) black contours denote the GPCP rainfall MJO anomalies (mm
day-1). For simplicity, only lags -4, -2, 0, +2, and +4 pentads of the MJO cycle are shown.
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435
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Figure 3: As Figure 2 but for the AIRS total ozone and TRMM rainfall MJO anomalies.
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Figure 4: Composite MJO cycles of the TOMS total ozone (DU, color shading) and the NCEP
200-hPa geopotential height (m, black contours) MJO anomalies.
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Figure 5: Composite MJO cycles of the NCEP 200-hPa stream function (106 m2 s-1, color
shading) and the NCEP 200-hPa geopotential height (m, black contours) MJO anomalies.
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