Chlorine partitioning near the polar vortex edge observed with ground-based FTIR and satellites at Syowa Station, Antarctica, in 2007 and 2011
- 1National Institute for Environmental Studies, Tsukuba, Ibaraki, 305-8506, Japan
- 2Graduate School of Environmental Studies, Tohoku University, Sendai, Miyagi, 980-8572, Japan
- 3Meteorological Research Institute, Tsukuba, Ibaraki, 305-0052, Japan
- 4National Institute of Polar Research, Tachikawa, Tokyo, 190-8518, Japan
- 5The Graduate University for Advanced Studies, Tachikawa, Tokyo, 190-8518, Japan
- 6University of Wollongong, Wollongong, New South Wales, 2522, Australia
- anow at: Weathernews Inc., Chiba, 261-0023, Japan
Correspondence: Hideaki Nakajima (email@example.com)
We retrieved lower stratospheric vertical profiles of O3, HNO3, and HCl from solar spectra taken with a ground-based Fourier transform infrared spectrometer (FTIR) installed at Syowa Station, Antarctica (69.0∘ S, 39.6∘ E), from March to December 2007 and September to November 2011. This was the first continuous measurement of chlorine species throughout the ozone hole period from the ground in Antarctica. We analyzed temporal variation of these species combined with ClO, HCl, and HNO3 data taken with the Aura MLS (Microwave Limb Sounder) satellite sensor and ClONO2 data taken with the Envisat MIPAS (the Michelson Interferometer for Passive Atmospheric Sounding) satellite sensor at 18 and 22 km over Syowa Station. An HCl and ClONO2 decrease occurred from the end of May at both 18 and 22 km, and eventually, in early winter, both HCl and ClONO2 were almost depleted. When the sun returned to Antarctica in spring, enhancement of ClO and gradual O3 destruction were observed. During the ClO-enhanced period, a negative correlation between ClO and ClONO2 was observed in the time series of the data at Syowa Station. This negative correlation was associated with the relative distance between Syowa Station and the edge of the polar vortex. We used MIROC3.2 chemistry–climate model (CCM) results to investigate the behavior of whole chlorine and related species inside the polar vortex and the boundary region in more detail. From CCM model results, the rapid conversion of chlorine reservoir species (HCl and ClONO2) into Cl2, gradual conversion of Cl2 into Cl2O2, increase in HOCl in the winter period, increase in ClO when sunlight became available, and conversion of ClO into HCl were successfully reproduced. The HCl decrease in the winter polar vortex core continued to occur due to both transport of ClONO2 from the subpolar region to higher latitudes, providing a flux of ClONO2 from more sunlit latitudes into the polar vortex, and the heterogeneous reaction of HCl with HOCl. The temporal variation of chlorine species over Syowa Station was affected by both heterogeneous chemistries related to polar stratospheric cloud (PSC) occurrence inside the polar vortex and transport of a NOx-rich air mass from the polar vortex boundary region, which can produce additional ClONO2 by reaction of ClO with NO2. The deactivation pathways from active chlorine into reservoir species (HCl and/or ClONO2) were confirmed to be highly dependent on the availability of ambient O3. At 18 km, where most ozone was depleted, most ClO was converted to HCl. At 22 km where some O3 was available, an additional increase in ClONO2 from the prewinter value occurred, similar to the Arctic.
Discussion of the detection of the recovery of the Antarctic ozone hole as the result of chlorofluorocarbon (CFC) regulations has been attracting attention. The occurrence of the Antarctic ozone hole is predicted to continue at least until the middle of this century. The world's leading chemistry–climate models (CCMs) indicate that the multimodel mean time series of the springtime Antarctic total column ozone will return to 1980 levels shortly after the midcentury (about 2060) (WMO, 2019). In fact, the recovery time predicted by CCMs has a large uncertainty, and the observed ozone hole magnitude also shows year-to-year variability (e.g., see Figs. 4–6 in WMO, 2019). Although Solomon et al. (2016) and de Laat et al. (2017) reported signs of healing in the Antarctic ozone layer only in September, there is no statistically conclusive report on the Antarctic ozone hole recovery (Yang et al., 2008; Kuttippurath et al., 2010; WMO, 2019).
To understand ozone depletion processes in polar regions, understanding the behavior and partitioning of active chlorines () and chlorine reservoirs (HCl and ClONO2) is crucial. Recently, the importance of ClONO2 was reviewed by von Clarmann and Johansson (2018). The chlorine reservoir is converted to active chlorine that destroys ozone on polar stratospheric clouds (PSCs) and/or cold binary sulfate through heterogeneous reactions:
where g, s, and l represent the gas, solid, and liquid phases, respectively (Solomon et al., 1986; Solomon, 1999; Drdla and Müller, 2012; Wegner et al., 2012; Nakajima et al., 2016).
are responsible for additional chlorine activation. When solar illumination is available, Cl2, HOCl, and ClNO2 are photolyzed to produce chlorine atoms by reactions
The yielded chlorine atoms then start to destroy ozone catalytically through reactions (Canty et al., 2016):
There are three types of PSCs, i.e., nitric acid trihydrate (NAT), supercooled ternary solution (STS), and ice PSCs. When the stratospheric temperatures get warmer than NAT saturation temperature (about 195 K at 50 hPa) and no PSCs are present, deactivation of chlorine starts to occur. Reformation of ClONO2 and HCl mainly occurs through reactions (Santee et al., 2008; Grooß et al., 2011; Müller et al., 2018)
The reformation of ClONO2 by Reaction (R12) from active chlorine is much faster than that of HCl by Reactions (R13) and (R14) if enough NOx are available (Mellqvist et al., 2002; Dufour et al., 2006). But the formation rates of ClONO2 and HCl are also related to ozone concentration. Grooß et al. (1997) showed that HCl increases more rapidly in the Antarctic polar vortex than in the Arctic polar vortex due to lower ozone concentrations in the Antarctic polar vortex. Low ozone reduces the rate of Reaction (R8) and then the Cl∕ClO ratio increases. Low ozone also reduces the rate of the following reaction:
This makes the NO∕NO2 ratio high and increases the Cl∕ClO ratio using the following reaction:
A high Cl∕ClO ratio leads to rapid HCl formation by Reactions (R13) and (R14) and reduces the formation ratio of ClONO2 by Reaction (R12) (Grooß et al., 2011; Müller et al., 2018).
The processes of deactivation of active chlorine are different between typical conditions in the Antarctic and those in the Arctic. In the Antarctic, the temperature cools below the NAT PSC existence threshold (about 195 K at 50 hPa) in the whole area of the polar vortex in all years, and almost complete denitrification and chlorine activation occur (WMO, 2007), followed by severe ozone depletion in spring. In the chlorine reservoir recovery phase, HCl is mainly formed by Reaction (R13) due to the lack of ozone (typically less than 0.5 ppmv) using the mechanism described in the previous paragraph (Grooß et al., 2011).
On the other hand, in the Arctic, typically less PSC formation occurs in the polar vortex due to generally higher stratospheric temperatures (∼ 10–15 K on average) compared with that of Antarctica. Then only partial denitrification and chlorine activation occur in some years (Manney et al., 2011; WMO, 2014). In this case, some ozone and NO2 are available in the chlorine reservoir recovery phase. Therefore, the ClONO2 amount becomes higher than that of HCl after PSCs have disappeared due to the rapid Reaction (R12) (Michelsen et al., 1999; Santee et al., 2003), which results in an additional increase in ClONO2 than the prewinter value at the time of chlorine deactivation in spring (von Clarmann et al., 1993; Müller et al., 1994; Oelhaf et al., 1994). In this way, the partitioning of the chlorine reservoir in springtime is related to temperature, PSC amounts, ozone, and NO2 concentrations (Santee et al., 2008; Solomon et al., 2015).
In the polar regions, the ozone and related atmospheric trace gas species have been intensively monitored by several measurement techniques since the discovery of the ozone hole. These measurements consist of direct observations by high-altitude aircraft (e.g., Anderson et al., 1989; Ko et al., 1989; Tuck et al., 1995; Jaeglé et al., 1997; Bonne et al., 2000), remote-sensing observations by satellites (e.g., Müller et al., 1996; Michelsen et al., 1999; Höpfner et al., 2004; Dufour et al., 2006; Hayashida et al., 2007), remote-sensing observations of OClO using a UV–visible spectrometer from the ground (Solomon et al., 1987; Kreher et al., 1996), and remote-sensing observations of ClO by a microwave spectrometer from the ground (de Zafra et al., 1989). Within these observations, ground-based measurements have the characteristic of high temporal resolution. In addition, the Fourier transform infrared spectrometer (FTIR) has the capability of measuring several trace gas species at the same time or in a short time interval (Rinsland et al., 1988). In this paper, we show the results of ground-based FTIR observations of O3 and other trace gas species at Syowa Station in the Antarctic in 2007 and 2011, combined with satellite measurements of trace gas species from the Microwave Limb Sounder on board the Aura satellite (Aura MLS) and Michelson Interferometer for Passive Atmospheric Sounding on board the European Environmental Satellite (Envisat MIPAS), to show the temporal variation and partitioning of active chlorine (ClOx) and chlorine reservoirs (HCl, ClONO2) from fall to spring during the ozone hole formation and dissipation period. In order to monitor the appearance of PSCs over Syowa Station, we used the Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) data on board the Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observations (CALIPSO) satellite. The methods of FTIR and satellite measurements are described in Sect. 2. The validation of FTIR measurements is described in Sect. 3. The results of FTIR and satellite measurements and discussion on the behavior of active and inert chlorine species using the MIROC3.2 chemistry–climate model are described in Sect. 4.
2.1 FTIR measurements
The Japanese Antarctic Syowa Station (69.0∘ S, 39.6∘ E) was established in January 1957. Since then, several scientific observations related to meteorology, upper atmospheric physics, glaciology, biology, geology, seismology, etc. have been performed. The ozone hole was first detected by Dobson spectrometer and ozonesonde measurements from Syowa Station in 1982 (Chubachi, 1984) and by Dobson spectrometer measurements at Halley Bay (Farman et al., 1985). We installed a Bruker IFS-120M high-resolution Fourier transform infrared spectrometer (FTIR) in the observation hut at Syowa Station in March 2007. This was the third high-resolution FTIR site in Antarctica in operation after the USA's South Pole Station (90.0∘ S) (Goldman et al., 1983, 1987; Murcray et al., 1987), the USA's McMurdo Station, and New Zealand's Arrival Heights facility at the Scott Base station (77.8∘ S, 166.7∘ E) (Farmer et al., 1987; Murcray et al., 1989; Kreher et al., 1996; Wood et al., 2002, 2004). The IFS-120M FTIR has a wavenumber resolution of 0.0035 cm−1, with two liquid-nitrogen-cooled detectors (with InSb and HgCdTe covering the frequency ranges 2000–5000 and 700–1300 cm−1, respectively) with six optical filters, and is fed by an external solar tracking system. One measurement takes about 10 min. At least six spectra were taken per day, covering each filter region. Since Syowa Station is located at a relatively low latitude (69.0∘ S) compared with McMurdo or Scott Base stations (77.8∘ S), there is an advantage of the short (about 1 month) polar night period, when we cannot measure atmospheric species using the sun as a light source. Since FTIR measurements at Syowa Station are possible from early spring (late July), FTIR can measure chemical species during ozone hole development. On the other hand, FTIR observations become possible only after September at McMurdo and Scott Base stations. Another advantage of Syowa Station is that it is sometimes located at the vortex boundary as well as inside and outside of the polar vortex, and this enables us to measure chemical species at different regions of polar chemistry related to the ozone hole. From March to December 2007, we made in total 78 d of FTIR measurements on sunny days. Another 19 d of FTIR measurements were performed from September to November 2011. After a few more measurements were performed in 2016, the FTIR was brought back to Japan in 2017. In Appendix A, Table A1 shows the days when FTIR measurements were made at Syowa Station with the information inside, in the boundary region, and outside of the polar vortex defined by the method described in Appendix B using ERA-Interim reanalysis data. Strahan et al. (2014) showed the year-to-year variation of Cly observed in the lower stratosphere of the Antarctic polar vortex. The Cly observed in 2007 (2.88 ppbv) was about +4.3 % more and that observed in 2011 (2.53 ppbv) was about −5.2 % less than the projected Cly from Newman et al. (2007) (2.76 ppbv for 2007 and 2.67 ppbv for 2011).
The retrieval of the FTIR spectra was done with the SFIT2 version 3.92 program (Rinsland et al., 1998; Hase et al., 2004). SFIT2 retrieves a vertical profile of trace gases using an optimal estimation formulation of Rodgers (2000), implemented with a semiempirical method which was originally developed for microwave measurements (Parrish et al., 1992; Connor et al., 1995). The SFIT2 forward model fully describes the FTIR instrument response, with absorption coefficients calculated using the algorithm of Norton and Rinsland (1991). The atmosphere is constructed with 47 layers from the ground to 100 km, using the FSCATM (Gallery et al., 1983) program for atmospheric ray tracing to account for refractive bending. The retrieval parameters for each gas, typical vertical resolution, and typical mean degrees of freedom for signal (DOFS) are shown in Table 1. Temperature and pressure profiles between 0 and 30 km are taken by the rawinsonde observations flown from Syowa Station on the same day by the Japanese Meteorological Agency (JMA), while values between 30 and 100 km are taken from the COSPAR International Reference Atmosphere 1986 (CIRA-86) standard atmosphere profile (Rees et al., 1990).
We retrieved vertical profiles of O3, HCl, and HNO3 from the solar spectra. We used monthly averaged ozonesondes profiles (0–30 km) and Improved Limb Atmospheric Spectrometer-II (ILAS-II) (Nakajima, 2006; Nakajima et al., 2006; Sugita et al., 2006) profiles (30–100 km) for the a priori profiles of O3, monthly averaged profiles from ILAS-II for HNO3, and monthly averaged profiles from HALOE (Anderson et al., 2000) for HCl. We focus on the altitude range of 15–25 km in this study. Typical averaging kernels of the SFIT2 retrievals for O3, HNO3, and HCl are shown in Fig. 1a, b, and c, respectively.
2.2 Satellite measurements
The Earth Observing System (EOS) MLS on board the Aura satellite was launched on 15 July 2004 to monitor several atmospheric chemical species in the upper troposphere to mesosphere (Waters et al., 2006). The Aura orbit is sun-synchronous at 705 km altitude, with an inclination of 98∘, 13:45 ascending (north-going) Equator-crossing time, and 98.8 min period. Vertical profiles are measured every ∼165 km along the suborbital track, the horizontal resolution is ∼ 200–600 km along track and ∼ 3–10 km across track, and the vertical resolution is ∼ 3–4 km in the lower-to-middle stratosphere (Froidevaux et al., 2006). ClO, HCl, and HNO3 profiles used in this study were taken from Aura MLS version 4.2 data (Livesey et al., 2006, 2018; Santee et al., 2011; Ziemke et al., 2011). Only daytime ClO data were used for the analysis. The daily MLS data within 320 km distance between the measurement location and Syowa Station were selected.
MIPAS is a Fourier transform spectrometer sounding the thermal emission of the earth's atmosphere between 685 and 2410 cm−1 (14.6–4.15 µm) in limb geometry (Fischer and Oelhaf, 1996; Fischer et al., 2008). The maximum optical path difference of MIPAS is 20 cm. The field of view of the instrument at the tangent points is about 3 km in the vertical and 30 km in the horizontal. In the standard observation mode in one limb scan, 17 tangent points are observed with nominal altitudes 6, 9, 12, 15, 18, 21, 24, 27, 30, 33, 36, 39, 42, 47, 52, 60, and 68 km. In this mode, about 73 limb scans are recorded per orbit. The measurements of each orbit cover nearly the complete latitude range from about 87∘ S to 89∘ N. MIPAS was placed on board Envisat, which was launched on 1 March 2002, and was put into a polar sun-synchronous orbit at an altitude of about 800 km with an inclination of 98.55∘ (von Clarmann et al., 2003). On its descending node, the satellite crosses the Equator at 10:00 local time. Envisat performs 14.3 orbits per day, which results in a good global coverage. The ClONO2 profiles which we used in this study were taken from Envisat MIPAS IMK/IAA version V5R_CLONO2_220 and V5R_CLONO2_222 (Höpfner et al., 2007). The daily MIPAS data within 320 km distance between the measurement location and Syowa Station were selected.
The CALIPSO satellite was launched on 28 April 2006. On the CALIPSO satellite, the CALIOP instrument was on board to monitor aerosols, clouds, and PSCs (Pitts et al., 2007). CALIOP is a two-wavelength, polarization-sensitive lidar that provides high-vertical-resolution profiles of the backscatter coefficient at 532 and 1064 nm, as well as two orthogonal (parallel and perpendicular) polarization components at 532 nm (Winker et al., 2007). In order to monitor the appearance of PSCs over Syowa Station, the daily CALIOP PSC data (Pitts et al., 2007, 2009, 2011) within 320 km distance between the measurement location and Syowa Station were selected.
We validated retrieved FTIR profiles of O3 with ozonesondes and Aura MLS version 3.3 data (Livesey et al., 2013) for 2007 measurements. Also, retrieved FTIR profiles of HNO3 and HCl were validated with Aura MLS data. We identified the nearest Aura MLS data from the distance between the Aura MLS tangent point and the point for the direction of the sun from Syowa Station at the time of the FTIR measurement at 20 km. The spatial and temporal collocation criteria used were within a 300 km radius and ±6 h. The ozonesonde and Aura MLS profiles were interpolated onto a 1 km grid and then smoothed using a 5 km wide running mean.
Figure 2a–b show absolute and relative differences of O3 profiles retrieved from FTIR measurements and those from model 1Z ECC-type ozonesonde measurements, respectively, calculated from 14 coincident measurements from 5 September to 17 December 2007. The typical precision and accuracy of the ECC-type ozone sondes are considered to be ± (3–5) % and ± (4–5) %, respectively (Komhyr, 1986). We define the relative percentage difference D as
The mean absolute difference between 15 and 25 km was within −0.02 to 0.40 ppmv. The mean relative difference D between 15 and 25 km was within −10.4 % to +24.4 %. The average of the mean relative differences D of O3 for the altitude of interest in this study (18–22 km) was +6.1 %, with the minimum of −10.4 % and the maximum of +19.2 %. FTIR data agree with validation data within root mean squares of typical errors in FTIR and validation data at the altitude of interest. Note that relatively large D values between 16 and 18 km are due to the small ozone amount in the ozone hole. Our validation results are quite comparable with the validation study at Izaña Observatory by Schneider et al. (2008).
Figure 2c–d show absolute and relative differences of O3 profiles retrieved from FTIR measurements and those from Aura MLS measurements, respectively, calculated from 33 coincident measurements from 1 April to 20 December 2007. The accuracy of MLS O3 data is reported to be 5 %–8 % between 0.5 and 46 hPa (Livesey et al., 2013). The mean absolute difference between 15 and 25 km was within −0.13 to +0.16 ppmv. The mean relative difference D between 15 and 25 km was within −16.2 % to +5.2 %. The average of the mean relative differences D for O3 for the altitude of interest in this study (18–22 km) was −5.5 %, with the minimum of −16.3 % and the maximum of +4.5%. Froidevaux et al. (2008) showed that Aura MLS is +8 % higher than the Atmospheric Chemistry Experiment Fourier transform spectrometer (ACE-FTS) at 70∘ S, which may explain the negative bias of FTIR data compared with MLS data.
Figure 2e–f show absolute and relative differences of HNO3 profiles retrieved by FTIR measurements and those from Aura MLS measurements, respectively, calculated from 47 coincident measurements from 25 March to 20 December 2007. The mean absolute difference between 15 and 25 km was within −0.56 to +0.57 ppbv. The mean relative difference D between 15 and 25 km was within −25.5 % to +21.9 %. The average of the mean relative differences D for HNO3 for the altitude of interest in this study (18–22 km) was +13.2 %, with the minimum of +0.2 % and the maximum of +21.9 %. This positive bias of FTIR data is still within the error bars of FTIR measurements. Livesey et al. (2013) showed that Aura MLS version 3.3 data have no bias within errors (∼ 0.6–0.7 ppbv (10 %–12 %) at a pressure level of 100–3.2 hPa) compared with other measurements. Livesey et al. (2018) showed no major differences between Aura MLS version 3.3 and version 4.2 data for HNO3.
Figure 2g–h show absolute and relative differences of HCl profiles retrieved by FTIR measurements and those from Aura MLS measurements, respectively, calculated from 50 coincident measurements from 25 March to 20 December 2007. The mean absolute difference between 15 and 25 km was within −0.20 to −0.09 ppbv. The mean relative difference D between 15 and 25 km was within −34.1 % to −3.0 %. The average of mean relative differences D for HCl for the altitude of interest in this study (18–22 km) is −9.7 %, with a minimum of −14.6 % and a maximum of −3.0 %. This negative bias of FTIR data is still within the error bars of FTIR measurements. Moreover, Livesey et al. (2013) showed that Aura MLS version 3.3 values are systematically greater than HALOE values by 10 %–15 % with a precision of 0.2–0.6 ppbv (10 %–30 %) in the stratosphere, which may partly explain the negative bias of FTIR data compared with MLS data. Livesey et al. (2018) showed no major differences between Aura MLS version 3.3 and version 4.2 data for HCl.
Table 2 summarizes the validation results of FTIR profiles compared with ozonesonde or Aura MLS measurements, as well as possible Aura MLS biases from the literature.
4.1 Time series of observed species
Figure 3a shows daytime hours at Syowa Station. Polar night ends at Syowa Station on 14 July (day 195). Figure 3b–e show the time series of temperatures at 18 and 22 km over Syowa Station using ERA-Interim data (Dee et al., 2011) for 2007 and 2011. Approximate saturation temperatures for NAT (TNAT) and ice (TICE) calculated by assuming 6 ppbv HNO3 and 4.5 ppmv H2O are also shown in the figures. The dates when PSCs were observed at Syowa Station identified by the nearest CALIOP data of that day were indicated by asterisks at the bottom of the figures. Over Syowa Station, PSCs were observed when temperature fell ∼4 K below TNAT. PSCs were often observed at 15–25 km from the beginning of July (day 183) to late August (day 241) in 2007 and from late June (day 175) to early September (day 251) in 2011.
PSCs were observed only at 18 km after August, due to the sedimentation of PSCs and downwelling of vortex air in late winter as is seen in Fig. 3. Although temperatures above Syowa Station were sometimes below TNAT-4 K in June and in late September, no PSC was observed during those periods. This may be due to other reasons, such as a different time history of temperature for PSC formation, and/or low HNO3 (denitrification) and/or H2O concentration (dehydration), which are needed for PSC formation in the late winter season (Saitoh et al., 2006).
Figures 4–7 show time series of HCl, ClONO2, ClO, , O3, and HNO3 over Syowa Station in 2007 and 2011 at altitudes of 18 and 22 km for all ground-based and satellite-based observations used in this study, respectively. O3 (sonde) is observed with the KC96 ozonesonde for 2007, which is different from the ones that were used for the validation in Sect. 3 and the ECC-1Z ozonesonde for 2011 by JMA (Smit and Straeter, 2004). HCl and HNO3 observed by Aura MLS and FTIR are plotted by different symbols. Total inorganic chlorine corresponds to the sum of HCl, ClONO2, and Clx, where the active chlorine species Clx is defined as the sum of ClO, Cl, and 2⋅Cl2O2 (Bonne et al., 2000). It is known that total inorganic chlorine has a compact relationship with N2O (Bonne et al., 2000; Schauffler et al., 2003; Strahan et al., 2014). Inferred total inorganic chlorine is calculated from the N2O value (in ppbv) measured by MLS and by using the empirical polynomial equation derived from the correlation analysis of Cly and N2O from the Photochemistry of Ozone Loss in the Arctic Region in Summer (POLARIS) mission which took place from April to September 1997 (Bonne et al., 2000). In order to compensate for the temporal trends of Cly and N2O values (2.90, 2.76, and 2.67 ppbv for Cly (Strahan et al., 2014) and 313, 321, and 324 ppbv for N2O (WMO, 2007, 2011, 2014) for the years 1997, 2007, and 2011, respectively), we used values 8 and 11 for constant A and 140 and 230 for constant B for years 2007 and 2011 in the following equation, respectively:
A transport barrier of minor constituents at the edge of the polar vortex was reported by Lee et al. (2001) and Tilmes et al. (2006). The distribution of minor constituents is quite different among the inside, in the boundary region, and outside of the polar vortex. In Figs. 4–7, the dark shaded area, the light shaded area, and the white area indicate the days when Syowa Station was located outside, in the boundary region, and inside of the polar vortex, respectively. In the Antarctic winter, there are often double peaks in the isentropic potential vorticity (PV) gradient with respect to equivalent latitude at the 450–600 K level (Tomikawa et al., 2015). The method to determine the three polar regions, i.e., inside the polar vortex, in the boundary region of the polar vortex, and outside the polar vortex, is described in Appendix B. Note that the Syowa Station is often located near the vortex edge, and the temporal variations of chemical species observed over Syowa Station reflect the spatial distributions as well as local chemical evolution. When Syowa Station was located at the boundary region or outside the polar vortex (e.g., day 310–316 in Fig. 4, day 192–195 in Fig. 5, day 309–316 in Fig. 6, and day 276–282 in Fig. 7), chemical species showed different values compared with the ones inside the polar vortex. The lack of data for ClO and HCl (MLS) from day 195 to day 219, 2007, and ClONO2 from day 170 to day 216, 2007 (Figs. 4a and 6a), is due to unrealistic large error values in Aura MLS or Envisat MIPAS data products during these periods.
The altitude of 18 km was selected because it was one of the altitudes where nearly complete ozone loss occurred. The altitude of 22 km, where only about half of the ozone was depleted, was selected to show the difference in the behavior of chemical species from that at 18 km.
The general features of the chemical species observed inside the polar vortex at 18 and 22 km in 2007 and 2011 are summarized as follows: HCl and ClONO2 decreased first, and then ClO started to increase in winter, while HCl increases and ClO decreases were synchronized in spring. HCl was almost zero from late June to early September, and the day-to-day variations were small over this period. HCl over Syowa Station indicates relatively larger values when it was located outside the polar vortex: for example, early August and the beginning of September at 22 km, 2007, in Fig. 6. HNO3 showed large decreases from June to July and then gradually increased in summer. Day-to-day variations of HNO3 from June to August were large. O3 decreased from July to late September when ClO concentration was increased. ClO was enhanced in August and September, and the day-to-day variations were large over this period. gradually increased in the polar vortex from late autumn to spring. The value became larger compared with its mixing ratio outside of the polar vortex in spring.
The following characteristics are evident at 18 km (Figs. 4 and 5). O3 gradually decreased from values of 2.5–3 ppmv before winter to values less than one-fifth, 0.3–0.5 ppmv, in October. The values of HCl from late June to early September were as small as 0–0.3 ppbv. The recovered values of HCl inside the vortex in spring (October–December) were larger than those before winter and those outside the polar vortex during the same period. ClONO2 inside the vortex kept near zero even after ClO disappeared and did not recover to the level before winter until spring.
At 22 km (Figs. 6 and 7), O3 gradually decreased from winter to spring, but the magnitude of the decrease was much smaller than that at 18 km. The values of HCl from late June to early September were 0–1 ppbv, which are larger than those at 18 km. The recovered values of HCl in spring were nearly the same as those before winter (around 2.2 ppbv). ClONO2 recovered to larger values than those before winter after ClO disappeared.
As for the temporal increase in ClONO2 in spring during the ClO decreasing phase, we can see a peak of 1.5 ppbv at 18 km in 2011 and at 22 km in both 2007 and 2011 around 27 September (day 270), but we see no temporal increase in ClONO2 at 18 km in 2007.
Figure 7 shows that temporal ClO enhancement and decrease in O3, ClONO2, and HNO3 occurred in early winter (30 May–19 June; day 150–170) at 22 km in 2011. This small ozone depletion event before winter may be due to an air mass movement from the polar night area to a sunlit area at lower latitudes.
4.2 Time series of ratios of chlorine species
In order to discuss the temporal variations of the chlorine partitioning, the ratios of observed HCl, ClONO2, and ClO with respect to were calculated. Hereafter, we will discuss the ratios of chlorine species only for the cases when Syowa Station was located inside the polar vortex.
Figures 8 and 9 show the time series of the ratios of each chlorine species with respect to in 2007 (a) and in 2011 (b) at 18 and 22 km, respectively. In these plots, HCl data from Aura MLS were used. Note that light blue in these figures shows that either ClONO2 or ClO data were missing on that day, while dark blue shows that all three data sets were available on that day. For both 2007 and 2011 at 18 km (Fig. 8), was 0.6–0.8 and was 0.2–0.3 before winter (10–20 May; day 130–140). The ratio of HCl to was 3 times larger than that of ClONO2 at that time. increased to ∼0.5 during the ClO-enhanced period (the period when ClO values were more than 80 % of its maximum value: 18 August–17 September; day 230–260). was 0–0.2 and ClONO2/ was 0-0.6 during this same period. ClONO2 shows a negative correlation with ClO, while HCl remained low even when ClO was low during this period. This negative correlation is shown in Fig. 10. When ClO was enhanced, the O3 amount gradually decreased and finally reached <0.5 ppmv (>80 % destruction) in October (7 October; day 280) (see Figs. 4 and 5). The ratios to became 0.9–1.0 for HCl and 0–0.1 for ClONO2 after the recovery in spring (after 17 October; day 290), indicating that almost all chlorine reservoir species became HCl via Reactions (R13) and/or (R14), due to the lack of O3 and NO2 during this period. The sum ratios were around 0.5–0.8 at the time of the ClO-enhanced period. The remaining chlorine is thought to be either Cl2O2 or HOCl, which will be shown in model simulation result in Sect. 4.6. The sum ratio became close to 1 after the recovery period (after 7 October; day 280).
For both 2007 and 2011 at 22 km (Fig. 9), was 0.8–0.9 and was 0.2–0.3 before winter (20 April–20 May; day 110–140). The ratio of HCl to was 3 to 4 times larger than that of ClONO2. ClO/ increased to 0.5–0.7 during the ClO-enhanced period (8–28 August – day 220–240 in 2007; 18 August–7 September – day 230–250 in 2011). was 0–0.2 and was 0–0.6 during this period. ClONO2 shows a negative correlation with ClO, while HCl remained low even when ClO was low during this period as in the case at 18 km. The O3 amount gradually decreased during the ClO-enhanced period but the concentration remained at more than 1.5 ppmv (less than half destruction) at this altitude (see Figs. 6 and 7). When the ClO enhancement ended, the increase in both ClONO2 and HCl occurred simultaneously in early spring (17 September–7 October; day 260–280). Then the ratios to became 0.6–0.7 for HCl and 0.3–0.4 for ClONO2 in spring (after 7 October; day 280). This phenomenon shows that more chlorine deactivation via Reaction (R12) occurred towards ClONO2 at 22 km rather than at 18 km. This is attributed to the existence of O3 and NO2 during this period at 22 km, which was different from the case at 18 km. The sum ratios were around 0.7–1.2 at the time of the ClO-enhanced period. The remaining chlorine is thought to be either Cl2O2 or HOCl. The sum ratio became around 1.2 after the recovery period (after 27 September; day 270). The reason why the observed sum ratio exceeds the calculated value might be because the N2O–Cly correlation from the one in Eq. (2) is not applicable at this altitude.
In 2011 at 18 km (Fig. 8), another temporal increase in ClONO2 up to a ratio of 0.4 occurred in early spring (around 2–12 October; day 275–285) in accordance with the HCl increase, and then the ClONO2 amount gradually decreased to nearly zero after late October (after 27 October; day 300). This temporal increase in ClONO2 could be attributed to the temporal change of the location of Syowa Station with respect to the polar vortex. Although Syowa Station was judged to be inside the polar vortex during 14 July–16 December (day 195–350) by our analysis, the difference between the equivalent latitude over Syowa Station and that at the inner edge became less than 10∘ on around 7 October (day 280), while it was typically between 15 and 20∘ on other days. O3 and HNO3 showed higher values around 7 October (day 280) (see Fig. 5), indicating that Syowa Station was located close to the boundary region during this period (see Fig. B2 in Appendix B). Therefore, the temporal increase in ClONO2 in 2011 at 18 km was attributed to spatial variation, not to chemical evolution.
4.3 Correlation between ClO and ClONO2
Figure 10 shows the correlation between ClO and ClONO2 during the ClO-enhanced period (8 August–17 September; day 220–260) at 18 km in 2007 (a) and 2011 (b) and at 22 km in 2007 (c) and 2011 (d). In this plot, the location of Syowa Station with respect to the polar vortex (inside, in the boundary region, and outside of the polar vortex) is indicated by different symbols. Note that MLS ClO and MIPAS ClONO2 data were sampled on the same day at the nearest orbit to Syowa Station for both satellites. The maximum differences between these two satellites' observational times and locations are 9.0 h in time and 587 km in distance. Mean differences are 6.8 h in time and 270 km in distance, respectively. Solid lines show regression lines obtained by reduced major axis (RMA) regression. Negative correlations of slope of about −1.0 between ClO and ClONO2 are seen in all figures.
The negative correlation between ClO and ClONO2 at Syowa Station is explained by the difference in the concentration of ClO, NO2, ClONO2, and HNO3 inside, outside, and at the boundary region of the polar vortex around the station. Outside of the polar vortex, the ClO concentration is lower and NO2 concentration is higher than those inside the polar vortex. Inside the polar vortex, HNO3 is taken up by PSCs and removed by the sedimentation of PSCs from the lower stratosphere (denitrification process). The NOx concentration is low because HNO3 is a reservoir of NOx through the reactions
The NO2 concentration is low and ClONO2 concentration is also low due to the consumption of ClONO2 by the heterogeneous Reaction (R2) inside the polar vortex. In spring, the ClO amount increases due to the activation of chlorine species by Reactions (R1)–(R8) inside the polar vortex. At the boundary region, ClO and NO2 concentrations indicate the value between the inside and outside of the polar vortex; that is, the ClO concentration is much higher than that outside of the polar vortex and NO2 concentration is much higher than that inside of the polar vortex. Thus, the ClONO2 concentration there is elevated in August–September due to Reaction (R12). This causes the negative correlation between ClO and ClONO2 due to the relative distance between Syowa Station and the edge of the polar vortex. When Syowa Station was located deep inside the polar vortex, there was more ClO and less ClONO2. On the contrary, when Syowa Station was located near the vortex edge, there was less ClO and more ClONO2. The equivalent latitude (EL) over Syowa Station was calculated as described in Appendix B for each correlation point. The EL at each correlation point is now shown by the color code in Fig. 10. It generally shows the tendency that warm-colored higher equivalent latitude points are located more towards the bottom right-hand side. This is further confirmed by three-dimensional model simulation as shown later.
4.4 Comparison with model results
Figures 11 and 12 show comparisons of daily time series of simulated mixing ratios of ClO, HCl, ClONO2, Cly, and O3 by the MIROC3.2 chemistry–climate model (Akiyoshi et al., 2016) with FTIR, Aura MLS, and Envisat MIPAS measurements at 18 and 22 km. For a description of the MIROC3.2 CCM, please see Appendix A. In these figures, Cly for Aura MLS in the panels (d) and (i) actually represents the value calculated by Eq. (2) using the N2O value measured by Aura MLS. Cly from the MIROC3.2 CCM is the sum of total reactive chlorines; i.e., . Note that we plotted modeled values at 12:00 UTC (∼ 15:00 local time of Syowa Station) calculated by the MIROC3.2 CCM in order to compare the daytime measurements of FTIR and satellites. In Fig. 11b, d, g, and i, modeled HCl and Cly are systematically smaller by 20 %–40 % compared with FTIR or MLS measurements. The cause of this discrepancy may be partly due to either smaller downward advection and/or faster horizontal mixing of an air mass across the subtropical barrier in MIROC3.2 CCM (Akiyoshi et al., 2016). Nevertheless, evolutions of measured ClO and ClONO2 for the period are well simulated by the MIROC3.2 CCM. Modeled O3 were in very good agreement with FTIR and/or MLS measurements throughout the year in both altitudes for both years. Hereafter, the result of MIROC3.2 CCM at 50 hPa (∼18 km) is discussed.
4.5 Polar distribution of minor species
Figure 13 shows distributions of temperature from the model nudged toward the ERA-Interim data and simulated mixing ratios of O3, NO2, HNO3, ClO, HCl, and ClONO2 by the MIROC3.2 CCM at 50 hPa for 24 June (day 175), 2 September (day 245), 6 September (day 249), and 6 October (day 279) in 2007. Polar vortex edges defined by the method described in Appendix B were plotted with white outlines. The location of Syowa Station is shown by a white star in each panel. On 24 June (day 175), stratospheric temperatures over Antarctica were already low enough for the onset of heterogeneous chemistry. Consequently, NO2 was converted into HNO3 via Reaction (R17), and HNO3 in the polar vortex was condensed onto PSCs. Note that the depleted area of NO2 was greater than that of HNO3. This is due to the occurrence of Reaction (R12) that converts ClO and NO2 into ClONO2 at the edge of the polar vortex, which is shown by the enhanced ClONO2 area at the vortex edge in Fig. 13. Also, HCl and ClONO2 are depleted in the polar vortex due to the heterogeneous Reactions (R1), (R2), (R3), and (R4) on the surface of PSCs and aerosols. Some HCl remains near the core of the polar vortex, because the initial amount of the counterpart of the heterogeneous Reaction (R1) (ClONO2) was less than that of HCl, as was also shown by CLaMS, SD-WACCM, and TOMCAT/SLIMCAT model simulations by Grooß et al. (2018). The O3 amount was only slightly depleted within the polar vortex on this day.
On 2 September (day 245), amounts of NO2, HNO3, HCl, and ClONO2 all show very depleted values in the polar vortex. The amount of ClO shows some enhanced values inside the polar vortex. The development of ozone depletion was seen in the polar vortex. Note that ClONO2 shows enhanced values around the boundary region of the polar vortex. This might be due to Reaction (R12) at this location. On this day (day 245), Syowa Station was located inside the polar vortex close to the vortex edge, where ClO was smaller and ClONO2 was greater than the values deep inside the polar vortex as observed and indicated by the upper-left circle with a cross in Fig. 10a.
On 6 September (day 249), most features were the same as on 2 September, but the shape of the polar vortex was different. Consequently, Syowa Station was located deep inside the polar vortex, where ClO was greater and ClONO2 was smaller than the values around the boundary region of the polar vortex as observed and indicated by the lower-right circle with a cross in Fig. 10a. Hence, the negative correlation between ClO and ClONO2 seen in Fig. 10 was due to variation of the relative distance between Syowa Station and the edge of the polar vortex.
As for HCl, it remained near zero not only on this day (6 September) but also on 2 September when Syowa Station was located inside the polar vortex close to the vortex edge. Therefore, observed day-to-day variations of HCl were small and did not show any correlation with ClO (see Figs. 4–7). A possible explanation to keep a near zero HCl value close to the vortex edge is due to so-called “HCl null cycles”, which were started with Reaction (R13), proposed by Müller et al. (2018). This cycle is discussed later.
On 6 October (day 279), ClO enhancement has almost disappeared. Inside the polar vortex, O3, NO2, HNO3, and ClONO2 showed very low values. Ozone was almost fully destroyed at this altitude in the polar vortex. However, the amount of HCl increased deep inside the polar vortex. This might be due to the recovery of HCl by Reactions (R13) and/or (R14) deep inside the polar vortex, where there was no O3 or NO2 left and Reactions (R13) and/or (R14) were favored compared with Reaction (R12). Syowa Station was located deep inside the polar vortex, and the simulated and observed amounts of HCl were both more than 10 times greater than those of ClONO2 on this day (see Fig. 4).
Figure 14 shows distributions of temperature from the model nudged toward the ERA-Interim data and simulated mixing ratios of O3, NO2, HNO3, ClO, HCl, and ClONO2 by the MIROC3.2 CCM at 50 hPa for 5 July (day 186), 19 August (day 231), 21 August (day 233), and 9 October (day 282) in 2011. The polar vortex edges and location of Syowa Station were also plotted. On 5 July (day 186), the situation was similar to that of 24 June (day 175) in 2007. Note that the inner edge of the polar vortex was defined on this day. Syowa Station was located deeper inside the polar vortex on 5 July in 2011 than on 24 June in 2007, and the remaining HCl was observed by MLS (see Fig. 5).
On 19 August (day 231) and 21 August (day 233), the situations were similar to those of 2 September (day 245) and 6 September (day 249) in 2007, respectively. ClO and ClONO2 correlations on these days are also indicated by circles with crosses in Fig. 10b.
On 9 October (day 282), the situation was similar to that of 6 October (day 279) in 2007, but Syowa Station was located inside the polar vortex closer to the inner vortex edge than in 2007. The recovery of ClONO2 by Reaction (R12) was simulated and observed at Syowa Station in addition to the recovery of HCl by Reaction (R13) (see Fig. 8b), because there were some remaining O3 and NO2 air masses near the inner vortex edge (see Fig. 5). This shows the phenomena described on the last paragraph in Sect. 4.2.
4.6 Time evolution of chlorine species from CCM and discussion
Three-hourly time series of zonal-mean active chlorine species, Cl2O2 (b), Cl2 (c), ClO (d), and their sum () (a), HOCl (e), and chlorine reservoir species HCl (f) and ClONO2 (g) modeled by MIROC3.2 CCM at 68.4, 71.2, 76.7, and 87.9∘ S in 2007 are plotted in Fig. 15. The dates on which the distribution of each species is shown in Fig. 13 are indicated by vertical dotted lines. In Fig. 15, it is shown that HCl and ClONO2 rapidly decreased on around 10 May (day 130) at 87.9∘ S due to the heterogeneous Reaction (R1), when PSCs started to form in the Antarctic polar vortex (Fig. 15f and g). Consequently, Cl2 was formed (Fig. 15c). Similar chlorine activation was seen at 76.7∘ S about 5–10 d later than at 87.9∘ S. The decrease in HCl stopped when the counterpart of the heterogeneous Reaction (R1) (ClONO2) was missing on around 20 May (day 140). The continuous loss of HCl occurred from June to July (day 160–200). The possible cause of this loss will be discussed later. Gradual conversion from Cl2 into Cl2O2 (ClO dimer) was seen at all latitudes on around 30 May–9 June (day 150–160) (Fig. 15b and c) through Reactions (R5), (R8), and (R9). At 87.9∘ S, conversion from Cl2 to Cl2O2 was slow, due to the lack of sunlight, which is needed for Reaction (R5). The increase in ClO occurred much later in winter (9 July; day 190 or later), because sunlight is needed to form ClO by Reactions (R5) and (R8) in the polar vortex (Fig. 15d). Nevertheless, there were some enhancements of ClO in early winter, on 24 June (day 175), simulated at the edge of the polar vortex (Fig. 13) where there was some sunlight available due to the distortion of the shape of the polar vortex. The increase in ClO occurred from a lower latitude (68.4∘ S) on around 14 July (day 195) towards a higher latitude (87.9∘ S) on around 12 September (day 255) (Fig. 15d). Diurnal variation of ClO was also seen at latitudes between 68.4 and 76.7∘ S. When the stratospheric temperature increased above NAT saturation temperature on around 27 September (day 270) (Fig. 3b), chlorine activation ended, and ClO was mainly converted into HCl at all latitudes inside the polar vortex (Fig. 15d and f). This is because Reactions (R13) and/or (R14) occur more frequently than Reaction (R12) inside the polar vortex due to the depleted O3 amount there, as was described in Sect. 1 (Douglass et al., 1995). The increase in HOCl due to the heterogeneous Reaction (R2) on the surface of PSCs occurred gradually from June at lower latitudes (68.4 and 71.2∘ S) (Fig. 15e). It also occurred at 76.7∘ S from July and at 87.9∘ S from August. The cause of the HOCl increase at 87.9∘ S from August is not clear at the moment. In Fig. 15, the species which decreased at 87.9∘ S from August was Cl2 (Fig. 15c). If sunlight was available, Cl2 was converted into HOCl through Reactions (R5) and (R8) as well as the following reaction:
Here, HO2 was needed to yield HOCl. One possibility to yield HO2 in August is either one of the HCl null cycles C1 or C2 (see Appendix C) or one of the HCl destruction cycles C3 or C4 (see Appendix C), which was described in Müller et al. (2018). If the air mass at 87.9∘ S was located equatorward due to the obliqueness of the polar vortex a few days earlier, then sunlight may have been available and such reactions could yield HOCl at 87.9∘ S.
The continuous loss of HCl was seen at 87.9∘ S between 9 June (day 160) and 19 July (day 200) even after the disappearance of the counterpart of the heterogeneous Reaction (R1) (Fig. 15f). The cause of this continuous loss was unknown until recently, where a hypothesis was proposed that includes the effect of decomposition of particulate HNO3 by some processes like ionization of air molecules caused by galactic cosmic rays during the winter polar vortex or photolysis of dissolved HNO3 in PSC particles (Grooß et al., 2018). However, they concluded that these processes could not explain the HCl discrepancy between their models and observations. We consider that the continuous loss of HCl was caused by the mixing of ClONO2-containing air with the air at the core of the polar vortex, due to the excursions of air parcels in and out of sunlight during the winter caused by the distortion of the polar vortex, which photochemically resupply ClONO2 and HOCl. Our result was indicated by some sporadic increase in ClONO2 on around 7 June (day 158), 28 June (day 179), and 8 July (day 189) at 76.7∘ S as shown in Fig. 15g. We confirmed that the shapes of the polar vortex were rather distorted on these days. Subsequently, HCl losses were observed at 76.7 and 87.9∘ S during these episodes in Fig. 15f. Thus, the continuous loss of HCl at the most polar latitude (87.9∘ S) could be due to the gradual mixing of air within the polar vortex during the winter period, when the polar vortex was still strong.
The ClONO2 distribution on 24 June 2007 in Fig. 13 shows a peak at around the polar vortex outer edge (equivalent latitude of ∼62∘ S) where there was no HCl. We confirmed that such a peak continued to exist from the middle of June to the end of July, when sunlight was not available at a geographical latitude higher than 70∘ S due to polar night. However, a substantial amount of ClONO2 exists between an equivalent latitude of 62∘ S (polar vortex outer edge) and 70∘ S, mainly due to the distortion of the polar vortex and availability of O3. At 62∘ S equivalent latitude, the amount of ClONO2 has a peak around these days, while HCl amounts were low. At around 65–70∘ S, HCl was almost fully depleted. Therefore, if the air mass which contains some ClONO2 traveled poleward due to mixing, it could react with HCl by Reaction (R1) and continuously destroy HCl in the core of the polar vortex during the polar night in June and July. Another explanation for the loss of HCl is the heterogeneous Reaction (R4) on the surface of PSCs with HOCl. Spiky increases in HOCl at 76.7 and 87.9∘ S and a simultaneous decrease in HCl occurred on around 7 July (day 188) and 20 July (day 201) in Fig. 15e and f. The continuous loss of HCl at the core of the polar vortex in August and September was recently proposed by Müller et al. (2018), who proposed that HCl destruction cycles C3 and C4 (see Appendix C) are responsible for the decline of HCl in the vortex core. These chemical cycles also require sunlight to occur, which may not be available in June and July at the vortex core. Therefore, the distortion of the polar vortex is also important for that reaction to occur as well. We consider that the reactions of HCl with both ClONO2 and HOCl contribute the continuous loss of HCl during winter in the vortex core.
Recently, Solomon et al. (2015) discussed the race between chlorine activation and deactivation to maintain enhanced levels of active chlorine during the time period (September and early October) when rapid ozone loss occurs. Müller et al. (2018) proposed so-called HCl null cycles to maintain enhanced chlorine levels. They proposed a mechanism in which the formation of HCl (Reaction R13) is followed by the immediate reactivation of HCl by null cycles C1 and C2 (see Appendix C) (Müller et al., 2018). Our MIROC3.2 CCM model results support the mechanism by high ClO and HOCl levels in September as shown in Fig. 15d and e.
Lower stratospheric vertical profiles of O3, HNO3, and HCl were retrieved using SFIT2 from solar spectra taken with a ground-based FTIR installed at Syowa Station, Antarctica, from March to December 2007 and September to November 2011. This was the first continuous measurement of chlorine species throughout the ozone hole period from the ground in Antarctica. Retrieved profiles were validated with Aura MLS and ozonesonde data. The absolute differences between FTIR and Aura MLS or ozonesonde measurements were within measurement error bars at the altitudes of interest.
To study the temporal variation of chlorine partitioning and ozone destruction from fall to spring in the Antarctic polar vortex, we analyzed temporal variations of measured minor species using FTIR over Syowa Station combined with satellite measurements of ClO, HCl, ClONO2 and HNO3. When the stratospheric temperature over Syowa Station fell ∼4 K below NAT saturation temperature, PSCs started to form and the heterogeneous reaction between HCl and ClONO2 occurred, and eventually, in early winter, both HCl and ClONO2 were almost completely depleted at both 18 and 22 km. When the sun came back to the Antarctic in spring, enhancement of ClO and gradual O3 destruction were observed. During the ClO-enhanced period, a negative correlation between ClO and ClONO2 was observed in the time series of the data at Syowa Station. This negative correlation is associated with the relative distance between Syowa Station and the edge of the polar vortex.
To investigate the behavior of whole chlorine and related species inside the polar vortex and the boundary region in more detail, results of the MIROC3.2 CCM simulation were analyzed. The direct comparison between CCM results and observations shows good day-to-day agreement in general, although some species show systematic differences especially at 18 km. The modeled O3 is in good agreement with FTIR and satellite observations. Rapid conversion of chlorine reservoir species (HCl and ClONO2) into Cl2, gradual conversion of Cl2 into Cl2O2, increase in HOCl in the winter period, increase in ClO when sunlight became available, and conversion of ClO into HCl were successfully reproduced by the CCM. The HCl decrease in the winter polar vortex core continued to occur due to both transport of ClONO2 from the polar vortex boundary region to higher latitudes, providing a flux of ClONO2 from more sunlit latitudes into the polar vortex, and the heterogeneous reaction of HCl with HOCl. The temporal variation of chlorine species over Syowa Station was affected by both heterogeneous chemistries related to PSC occurrence inside the polar vortex and transport of a NOx-rich air mass from the polar vortex boundary region, which can produce additional ClONO2 via Reaction (R12).
The deactivation pathways from active ClO into reservoir species (HCl and/or ClONO2) were confirmed to be very dependent on the availability of ambient O3. At 18 km, where most ozone was depleted, most ClO was converted to HCl. At 22 km, when some O3 was available, an additional increase in ClONO2 than the prewinter value occurred, similar to the Arctic, through Reactions (R15) and (R12) (Douglass et al., 1995; Grooß et al., 1997).
The chemistry–climate model used in this study was the MIROC3.2 CCM, which was developed on the basis of version 3.2 of the Model for Interdisciplinary Research on Climate (MIROC3.2) general circulation model (GCM). The MIROC3.2 CCM introduces the stratospheric chemistry module of the old version of the CCM that was used for simulations proposed by the chemistry–climate model validation (CCMVal) and the second round of CCMVal (CCMVal2) (WMO, 2007, 2011; SPARC CCMVal, 2010; Akiyoshi et al., 2009, 2010). The MIROC3.2 CCM is a spectral model with a T42 horizontal resolution (2.8∘ × 2.8∘) and 34 vertical atmospheric layers above the surface. The top layer is located at approximately 80 km (0.01 hPa). Hybrid sigma–pressure coordinates are used for the vertical coordinate. The horizontal wind velocity and temperature in the CCM were nudged toward the ERA-Interim data (Dee et al., 2011) to simulate global distributions of ozone and other chemical constituents on a daily basis. The transport is calculated by a semi-Lagrangian scheme (Lin and Rood, 1996). The chemical constituents included in this model are Ox, HOx, NOx, ClOx, BrOx, hydrocarbons for methane oxidation, heterogeneous reactions on the surface for sulfuric acid aerosols, supercooled ternary solutions, nitric acid trihydrate, and ice particles.
The CCM contains 13 heterogeneous reactions on multiple aerosol types (Akiyoshi, 2007) as well as gas-phase chemical reactions and photolysis reactions. The surface of the particles for the heterogeneous reactions is calculated from the volume of condensation, assuming number density of the particles and the size distributions. Additionally, sedimentation of the particles is considered. The reaction-rate and absorption coefficients are based on JPL-2010 (Sander et al., 2011). The family method is used to calculate gas-phase chemical reactions. The time integrations for the families and heterogeneous reactions are performed explicitly. The time step for the chemistry scheme is 6 min. A scheme of spherical geometry for radiation transfer was developed (Kurokawa et al., 2005) and used for radiation transfer calculation in the CCM. The photolysis rates of chemical constituents are calculated online, using the radiation flux in the CCM with 32 spectral bins. All the 42 photolysis reactions, 140 gas-phase reactions, and 13 heterogeneous reactions are summarized in Table A2. See Akiyoshi et al. (2016) and the Supplement of Morgenstern et al. (2017) for more details.
Total: 42 photolysis reactions, 140 gas-phase reactions, and 13 heterogeneous reactions.
The inner and outer edges of the polar vortex were determined as follows.
Equivalent latitudes (ELs) (McIntyre and Palmer, 1984; Butchart and Remsberg, 1986) were computed based on isentropic potential vorticity at 450 and 560 K isentropic surfaces for 18 and 22 km, respectively, using the ERA-Interim reanalysis data (Dee et al., 2011).
Inner and outer edges (at least 5∘ apart from each other) of the polar vortex were defined by local maxima of the isentropic potential vorticity gradient with respect to equivalent latitude only when a tangential wind speed (i.e., mean horizontal wind speed along the isentropic potential vorticity contour; see Eq. 1 of Tomikawa and Sato, 2003) near the vortex edge exceeds a threshold value (i.e., 20 m s−1; see Nash et al., 1996, and Tomikawa et al., 2015).
Then, the polar region was divided into three regions – i.e., inside the polar vortex (inside of inner edge), in the boundary region of the polar vortex (between the inner and outer edges), and outside the polar vortex (outside of outer edge) – when there were two polar vortex edges. When there was only one edge, the polar region was divided into two regions: i.e., inside the polar vortex and outside the polar vortex.
Figures B1 and B2 show time-equivalent latitude sections of modified potential vorticity (MPV) and its gradient with respect to EL at 450 and 560 K isentropic potential temperature (PT) surfaces in 2007 and 2011, respectively. MPV is a scaled PV to remove its exponential increase with height (cf., Lait, 1994). The inner and outer edge(s) are plotted by black dots, while the ELs of Syowa Station on those days are plotted by red dots. It can be seen that inner edges were first formed at an EL of around 70∘ in April, and outer edges started to form at an EL of around 55∘ in July–August, forming the boundary region. Then, those two edges converge into one edge at an EL of around 60∘ in November. Finally, the polar vortex edge disappeared in December. Syowa Station was mostly located inside the polar vortex, but it was sometimes located at the boundary region or outside the polar vortex, depending on different PT levels.
In Müller et al. (2018), new chemical cycles C1 and C2 were proposed to maintain high levels of active chlorine in the Antarctic spring, referred to as HCl null cycles, as follows:
Also, other chemical cycles which are responsible for the decline of HCl during Antarctic August and September, referred to as HCl destruction cycles, are also proposed by Müller et al. (2018) as follows:
The FTIR data presented here can be obtained from the Global Environmental Database at the National Institute for Environmental Studies in electronic form (HDF files) from the following DOIs:
https://doi.org/10.17595/20190911.001 (FTIR data for 2007; Nakajima, 2019a),
https://doi.org/10.17595/20190911.002 (FTIR data for 2011; Nakajima, 2019b).
The MIROC3.2 CCM outputs are from the REF-C1SD simulation data from the CCMI, which are stored at the CCMI site of the Centre for Environmental Data Analysis at the National Centre for Earth Observation at http://data.ceda.ac.uk/badc/wcrp-ccmi/data/CCMI-1/output/NIES/CCSRNIES-MIROC3.2 (last access: 21 January 2020).
The MLS data were taken from NASA's Earthdata page at the Goddard Space Flight Center at the following site: https://disc.gsfc.nasa.gov/datasets?page=1&keywords=AURA MLS (last access: 21 January 2020; Earth Data, 2020).
The MIPAS data were taken from the Institute of Meteorology and Climate Research at the Karlsruhe Institute of Technology at the following site: http://www.imk-asf.kit.edu/english/308.php (last access: 21 January 2020).
The CALIOP data were taken from NASA's Langley Research Center data center at the following site: https://www-calipso.larc.nasa.gov/resources/calipso_users_guide/data_summaries/psc/index.php (last access: 21 January 2020; National Aeronautics and Space Administration, 2020).
HN, IM, YN, and MT conceived and worked on the current research project. HN, KS, and TK made FTIR observations at Syowa Station in 2007 and 2011. HN, YN, KS, and NBJ conducted the SFIT2 retrievals. HA conducted MIROC3.2 CCM simulations and ED analyzed them. YT performed the polar vortex categorization calculation. HN, IM, YN, HA, YT, and NBJ contributed to the interpretation of the results and wrote the paper.
The authors declare that they have no conflict of interest.
We acknowledge all the members of the 48th Japanese Antarctic Research Expedition (JARE-48) and JARE-52 for their support in making the FTIR observation at Syowa Station. The data provision of Aura MLS, Envisat MIPAS, and CALIPSO CALIOP is much appreciated. We thank the Japan Meteorological Agency for providing the ozonesonde and rawinsonde data at Syowa Station. Thanks are due to Yosuke Yamashita for performing the CCM run. The model computations were performed on NEC-SX9/A(ECO) and NEC SX-ACE computers at the CGER, NIES. We thank Takafumi Sugita for useful discussion and comments. We also thank the three anonymous referees for their useful comments, which significantly improved the contents of this paper.
The model computations in this research has been supported by the Ministry of the Environment, Japan (grant no. 2-1303), and the Environment Restoration and Conservation Agency, Japan (grant no. 2-1709).
This paper was edited by Farahnaz Khosrawi and reviewed by three anonymous referees.
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