Strong downdrafts preceding rapid tropopause ascent and their potential to identify cross-tropopause stratospheric intrusions
The capability of measuring three-dimensional wind and tropopause structure with relatively high time and vertical resolution makes very-high-frequency (VHF) radars a potentially important tool for studying various processes of the atmosphere. However, at present several unanswered questions remain regarding the use of VHF radars to identify possible stratospheric intrusions. Here the potential detection of stratospheric intrusion events is discussed using the Beijing MST (mesosphere–stratosphere–troposphere) radar located at Xianghe (39.75∘ N, 116.96∘ E). During the passage of a cutoff low in late November 2014, a deep V-shaped tropopause structure and strong downdrafts (> 0.8 m s−1) immediately preceding the rapid tropopause ascent (> 0.2 km h−1) were observed. Within the height region of the downdrafts, the stability of the radar tropopause seems to be weakened. Analysis results from global reanalysis and the satellite data, as well as the trajectory model, have shown clear evidence of downward stratospheric intrusions (dry ozone-rich and depleted methane air) associated with the strong downdrafts. A total of 20 typical cases of such strong downdrafts, occurring during various synoptic processes in different seasons, have been presented, and 15 of them are exactly associated with some form of stratospheric intrusions. Four years (2012–2015) of such downdrafts are further discussed. The observations reveal that the strong downdrafts preceding the rapid tropopause ascent can be a valuable diagnostic for monitoring intrusion events, which helps us to gain a better understanding of stratospheric intrusions in VHF radar observations.
The tropopause is a stable transition zone separating the stably stratified stratosphere from the active free troposphere. The stratospheric and tropospheric air are remarkably different in their chemical and dynamical characteristics. The stratosphere is dominantly high in ozone and potential vorticity (PV) content and low in water vapor (WV) and methane (CH4) concentration, while the troposphere is the opposite (Holton et al., 1995). Consequently, the natural stable tropopause layer, characterized by strong gradients of trace constituents and wind speeds, plays an important role in stratosphere–troposphere exchange (STE) processes. In other words, the layer is a significant barrier for the atmospheric transport between stratosphere and troposphere (Mahlman, 1997). From a long-term point of view, the seasonal variation of the tropopause height determines the seasonal variation of the flux of stratospheric air into the free troposphere (Appenzeller et al., 1996). Under global climate warming (e.g., the continuing rise in CO2), the tropopause variation is also a significant factor that must be considered with regards to the recovery of the stratospheric ozone (Butchart et al., 2010; Chipperfield et al., 2017). On the other hand, the short-term tropopause variability is sensitive to various mesoscale and small-scale atmospheric processes, during which the folding or intrusion events commonly occur. This characteristic of the tropopause change is sometimes directly used to detect the tropopause folds (e.g., Rao et al., 2008; Alexander et al., 2012, and references therein), but is less often, if at all, directly used to identify stratospheric intrusions. More detailed analysis of the variability of high-resolution tropopause height and of course some other parameters (e.g., three-dimensional wind), and how the stratospheric air is transported across the tropopause into the troposphere, will help us to obtain a better understanding of the downward stratospheric intrusions (e.g., Sprenger et al., 2003; Leclair de Bellevue et al., 2007; Das et al., 2016).
Although photochemical production within the troposphere is the main source of tropospheric ozone, the influence of downward stratospheric intrusions on tropospheric ozone content cannot be ignored (Oltmans and Levy II, 1992; Stevenson et al., 2006). Stratospheric intrusions bring dry ozone-rich air down into the free troposphere (e.g., Stohl et al., 2000; Sørensen and Nielsen, 2001) and sometimes even deep to the surface (e.g., Gerasopoulos et al., 2006; Grant et al., 2008; Jiang et al., 2015; Das et al., 2016). By now, it is well established that these intrusions of stratospheric origin will significantly influence other trace gases (such as hydroxyl (OH)) in the troposphere (Holton et al., 1995). These influences then will further contribute to the change of radiative balance (Ramaswamy et al., 1992) and play an important role in the radiative forcing of global climate change (Holton et al., 1995). It is true that stratospheric intrusion events occur all over the world and in any season. However, they are highly episodic in both vertical and isentropic (horizontal) directions (Chen, 1995). Various dynamical and physical processes have been proposed to be responsible for extratropical intrusion events. These mainly include tropopause folds, stratospheric streamers and break-up, cutoff lows (COLs), wave breaking, and mesoscale convective activities and thunderstorms (Stohl et al., 2003).
The certain dynamical and chemical characteristics of stratospheric air allow the tracers, such as dry ozone-rich and high PV, to be proper indicators for the intrusions penetrating down into the troposphere. Based on these tracers, various tools are available to detect intrusion events. Balloon-borne ozonesonde sounding is an effective tool to make measurements of ozone with high vertical resolution, but is limited by coverage (He et al., 2011) and temporal resolution. In contrast, the satellite-borne remote sensing instruments, such as the Atmospheric Infrared Sounder (AIRS), can provide nearly global coverage of various trace gases but have limitations in vertical and temporal resolution. Another method for studying transport processes is the trajectory model, from which the backward trajectories can provide valuable information on the possible sources of the trace gases (e.g., Elbern et al., 1997).
By far, large-scale STE has been widely studied and is fairly well understood, but the details of small-scale intrusions still need more research (e.g., Holton et al., 1995). Kumar and Uma (2009) reported that the shortage of direct measurements of vertical winds near the tropopause may be responsible for the lack of fine-scale observations of smaller scale intrusions.
Very-high-frequency (VHF) radars, compared to the tools mentioned above, are capable of continuously monitoring the atmosphere under any weather conditions and detecting tropopause height from backscattered signal with both high temporal and spatial resolution. During the past two decades, VHF radar measurements have commonly been used to assist in the study of stratospheric intrusions (e.g., Hocking et al., 2007; Das et al., 2016). However, it still remains uncertain in many aspects when only using the VHF radar to identify intrusion events, especially the criteria for the identification. Complicated and changeable atmospheric processes make it difficult to identify the intrusion events by only radar data. Hocking et al. (2007) reported that the rapid ascent in radar-derived tropopause (RT) altitude (> 0.2 km h−1) can be a valuable diagnostic for possible stratospheric intrusions. Their observation results clearly indicate that almost every occurrence of definite stratospheric intrusion is related to a definite RT ascent (> 0.2 km h−1, occurred at or just before the intrusion). The reverse is also reasonable; that is, almost every occurrence of definite RT ascent is associated with some form of intrusion (Hocking et al., 2007). Please note that we do not mean that the tropopause ascent is the best and most accurate diagnostic that can be used directly for identifying possible intrusions. As motivated by the study of Hocking et al. (2007), tropopause ascent is one of the key objects in this study.
Only using the information of RT height variability is, of course, insufficient for quantifying intrusion events accurately using radar data. Therefore, radar measurements of vertical motions are also considered simultaneously to discuss the possible capability of radar measurements for identifying cross-tropopause stratospheric intrusions, which is the main point of this paper. This study is carried out mainly via a detailed case observation during a COL passage and 20 other general cases during various synoptic situations. In Sect. 2 the datasets used in this paper are described, Sect. 3 presents detailed results and discussion, and Sect. 4 gives the conclusions.
2.1 MST radar data and tropopause detection
The Beijing MST (mesosphere–stratosphere–troposphere) radar located at Xianghe, China (39.75∘ N, 116.96∘ E; 22 m above sea level), is a VHF radar operated at 50 MHz and installed in 2010 based on the first phase of Chinese Meridian Space Weather Monitoring Project (Chinese Meridian Project for short) (Wang, 2010). The radar antenna array consists of a 24×24 three-element Yagi antenna to produce an average power aperture product of 3.2×108 Wm2 and maximum directive gain of 34.8 dB. It operates radiation pattern with 172 kW peak power and 3.2∘ half-power beam width. More detailed information of the radar system can be found in Chen et al. (2016). Routine low-mode data were used for present study with 0.5 h time resolution and 1 µs coded pulse, which provides 150 m vertical resolution. Details of the low-mode setup used in this study are given in Table 1.
It has long been known that VHF radar reflectivity is proportional to the mean generalized refractive index gradient M, which is a function of humidity variation and static stability and is given by Ottersten (1969) as follows:
where p is the atmospheric pressure (hPa), T is the temperature (K), θ is the potential temperature (K), and q is the specific humidity (gg−1). According to the second and third terms of Eq. (1), large humidity variation contributes to the echo from the lower and middle troposphere. From the first term, the radar backscatter power is proportional to the static stability, which in fact is directly proportional to the potential temperature gradient. The tropopause, near which a strong potential temperature gradient exists, will lead to strong radar echoes in vertical incidence, as well as large radar aspect sensitivity (as shown in Fig. 1). Radiosonde data used in this paper were received from the GTS1 type digital radiosonde launched from Beijing Meteorological Observatory (39.93∘ N, 116.28∘ E; station number 54511), which is less than 45 km away from the MST radar site. The black line in Fig. 1 denotes the lapse-rate tropopause (LRT) defined using the temperature lapse rate (World Meteorological Organization, 1986). Applying the characteristic (enhanced radar echoes due to partial specular reflection) mentioned above, the tropopause can be detected and its height determined by VHF radars (Gage and Green, 1979). It has received widespread application around the world, in middle latitudes (e.g., Hocking et al., 2007), polar regions (e.g., Alexander et al., 2012), and tropical regions (e.g., Yamamoto et al., 2003; Das et al., 2008). Here, the radar-determined tropopause (RT) height is defined as the height (above 500 hPa) at which the maximum vertical gradient of echo power is located (shown as the orange circle in Fig. 1a). This definition of RT is similar to that in the studies of Alexander et al. (2012) and Ravindrababu et al. (2014).
In the present study, the MST radar mainly provides continuous measurements of backscattered echo power, three-dimensional wind, and RT height with a time resolution of 0.5 h. In addition, the radar aspect sensitivity, expressed as the ratio between vertical (pv) and oblique (po; here 15∘ north is used) beam echo power, is mainly caused by the horizontally stratified anisotropic stable air and thus will be used as a potential signature of stratospheric intrusions in the troposphere (e.g., Kim et al., 2001). The backscattered echo power given here is expressed as relative power in decibels (dB). In order to reduce the random noise, the profile of pv is smoothed by a three-point running mean in altitude. Note that the data that are heavily contaminated will be eliminated from our datasets. The data of December 2015 and September 2015 are excluded.
2.2 AIRS satellite data
The AIRS instrument on the NASA Aqua/EOS polar orbit satellite is a 2378-channel nadir cross-track scanning infrared spectrometer. It can provide profiles of a number of trace gases, including ozone and CH4 (Susskind et al., 2003). The footprint of these retrieval data is 45 km by 45 km and their most sensitive region is in an altitude range of 300–600 hPa. Many studies have shown that these AIRS retrieval constituents are useful indicators for detecting stratospheric intrusions. He et al. (2011) suggested that AIRS can observe the enhanced tropospheric ozone that is of stratospheric origin. Xiong et al. (2013) reported that AIRS is capable of observing abnormal depletion in CH4 in the troposphere during intrusions. AIRS offers good latitude–longitude coverage. Here we use version 6 of the AIRS Level-3 ozone and methane retrieval products.
2.3 Meteorological reanalysis
European Centre for Medium-Range Weather Forecasts (ECMWF) reanalysis ERA-Interim data are also used. After November 2000 the data are based on the T511L60 version available with a 6 h temporal resolution and , latitude–longitude grid (Dee et al., 2011). The dataset from 15 isentropic and 37 pressure levels interpolated into a grid are applied for the present study.
2.4 HYSPLIT model
Backward (forward) trajectories in given starting locations are capable to reproduce the sources (destinations) of the air parcel that will allow us to examine the intrusions of stratospheric origin in the troposphere (e.g., Elbern et al., 1997). The Hybrid Single Particle Lagrangian Integrated Trajectory model (HYSPLIT) developed by the National Oceanic and Atmospheric Administration (NOAA) Air Resource Laboratory (ARL) (Rolph, 2003; Stein et al., 2016) is applied to calculate the backward and forward trajectories. The calculation method of the model is a hybrid between the Lagrangian approach and the Eulerian methodology. In this paper, Global Data Assimilation System (GDAS) datasets are adopted for driving the HYSPLIT.
3.1 Meteorological synoptic situation
On the morning of 29 November 2014, a 500 hPa trough developed on the western site of Lake Baikal (western Siberia). The trough moved southeastward and extended equatorward and its southern tip separated from the westerlies in the afternoon of 30 November 2014 (Fig. 2b), forming a COL near the radar site as shown by the closed geopotential contour. The black stars in Fig. 1 and other figures indicate the location of the radar site. On the following days, the COL system moved northeastward gradually (Fig. 2b) and finally stayed over eastern Russia near Sakhalin Island until it reconnected and merged to the westerly flow. 315 K isentropic PV patterns have shown the coarse-resolution features of intrusions from the polar reservoir across the tropopause into the midlatitude troposphere. The PV streamer curved and rolled up cyclonically along the western flank of the COL (Fig. 2b).
Figure 3 shows the time series of hourly surface meteorological parameters over the Beijing station. The data are obtained from the Chinese National Meteorology Information Center, less than 50 km from the MST radar site. As the dry cold air invasion accompanied by the COL traveled deeply into the planetary boundary layer, it brought severe weather to the surface, including a rapid decrease in temperature and humidity and a rapid increase in surface wind and sea level pressure. The humidity decreased from ∼85 % to 12 % within less than 8 h. It is well established that the polar-type COLs have strong potential to trigger deep convection (Price and Vaughan, 1993). To examine the potential convection, maps of high-quality Climate Data Record (CDR) of daily outgoing longwave radiation (OLR) (Lee, 2014) are displayed in Fig. 4. During the development of the COL, a local region with an abnormal low OLR value was clearly observed near the radar site on 29 November (Fig. 4b). The satellite-observed cloud top temperature also showed the low values corresponding to the low OLR (figure not shown), indicating that convection may be generated near the radar site on 29 November. Please note that we did not observe such a low value either in OLR (Fig. 4c, d) or in cloud top temperature near the radar site on 30 November and 1 December. The time for all the observations in this paper is shown in universal time (UTC) which is 8 h behind Beijing standard time (LT = UTC+8).
3.2 MST radar observations
Radar echo power, horizontal wind vector, vertical wind, and radar aspect sensitivity are plotted in Fig. 5 as a function of height and time during the passage of the COL. Time variation of RT (black line) and LRT (black crosses) heights are also displayed. The RT height first experienced a rapid descent, and then increased rapidly, forming a deep V-shaped structure of ∼4 km depth. The vertical velocity of the RT height variation (both the rapid descent and ascent branches) reaches up to 0.28 km h−1. The rapid RT variation in altitude is in fact the response of the tropopause fold below the jet stream, which is represented well in Fig. 8a. Rapid variation in RT height created a region with low echo power (marked by R on Fig. 5a) and low aspect sensitivity (marked by R′ on Fig. 5d), for which one would normally expect to find a high value within the “normal” tropopause layer. Unlike the RT height, the radiosonde LRT altitudes are nearly constant during the COL passage. In normal conditions, RT agrees well with the LRT altitude, such as indicated by Fig. 6a. However, large differences, of the order of 2.5 km (as shown in Fig. 6b at 12:00 UTC 30 November), are observed between LRT and RT in altitude during the passage of the COL as expected. It is the difference in definition that contributes most to the large differences, especially under the tropopause fold conditions (e.g., Yamamoto et al., 2003; Fukao et al., 2003). It is worth noting that, in Fig. 6b, although there is no clear reversion in the radiosonde temperature profile within the height of RT, the RT height corresponds well to the reversion of zonal and meridional wind and potential temperature gradient. Such differences between RT and LRT heights can commonly be observed, especially during extreme synoptic situations such as cyclones (e.g., Alexander et al., 2012).
The most important observation in this detailed case experiment is the strong downdrafts (hereinafter inferred to as main downdrafts) observed immediately preceding the rapid RT ascent (Fig. 5c). The radar echo power sharply weakened (dotted rectangle in Fig. 5a) and the wind direction changed rapidly (Fig. 5b; change from dominant southerly wind to dominant northerly jet) within the height region of the main downdrafts. As mentioned previously, an abnormal low value in OLR and cloud top temperature indicates the possible occurrence of convective activity on 29 November, but nothing significant appeared on 30 November near the radar site. Consequently, we preliminarily consider that the main downdrafts that occurred near 07:00 UT 30 November might not be produced directly by convective activity. Here, the accurate origin of the main downdrafts will not be discussed in detail, and it is also beyond the scope of present study.
The research by Hocking et al. (2007) has suggested that the rapid ascent in RT height (> 0.2 km h−1) can be a valuable diagnostic for the occurrence of stratospheric intrusions. Here in this paper, the main downdrafts preceding the rapid RT ascent observed by the Beijing MST radar are thus suspected to be an important feature or response of some form of vertical stratospheric intrusions. Firstly, as the tropopause descends (folded downward), it will displace stratospheric air into the troposphere (e.g., Hoskins et al., 1985). Secondly, the main downdrafts will act as an effective way to weaken the tropopause by means of continuously impinging on the tropopause, through which the stratospheric air is permitted to penetrate down into the free troposphere (e.g., Hirschberg and Fritsch, 1993; Kumar, 2006). In addition, after the main downdrafts, the observed region near the upper troposphere with strong backscatter echoes (marked by Q) and especially with abnormal high aspect sensitivity (marked by Q′) may also be a weak signature of the possible intrusions. In normal conditions, they are usually low in value in the upper troposphere (such as the region marked by P and P′). As we mentioned before, a large value in radar aspect sensitivity is mainly caused by reflection from the stable atmospheric layer, such as the tropopause or lower stratosphere. When stable stratospheric air intrudes into the troposphere and without mixing with the surrounding air mass, the intrusions in the free troposphere will be reflected as abnormal large aspect sensitivity. Further direct evidence of the relevant intrusions in dynamical and chemical aspects will be demonstrated in the next section, using satellite AIRS and global reanalysis data.
3.3 Associated stratospheric intrusions
Due to the sensitivity of the AIRS, retrieved ozone and CH4 is between 300 and 600 hPa. Figure 7 shows the 500 hPa distribution of AIRS-observed ozone and CH4, along with the AIRS tropopause contour (defined based on the temperature lapse rate). The ozone distribution maps (Fig. 7a and c) clearly show a large area with enhanced tropospheric ozone (> 80 ppbv) near the radar site during the passage of the COL. Moreover, severe CH4 depletion (< 1840 ppbv) was also observed (Fig. 7b and d). These features of the ozone enhancement, CH4 depletion, and the corresponding low tropopause altitude clearly support the evidence of vertical downward cross-tropopause stratospheric intrusions on 30 November.
The vertical cross section of ECMWF PV and specific humidity at 18:00 UT 30 November 2014 and the daily AIRS ozone on 30 November 2014, along a constant latitude 40∘ N, is shown in Fig. 8. Please note that the high PV and dry air have been observed intruding deep into the troposphere as low as 650 hPa (∼3.6 km), whereas the vertical structure of AIRS ozone has shown that the enhanced ozone intruded into the troposphere at ∼500 hPa. This difference in vertical scale of intrusion between ozone and PV parameters is most likely due to two reasons: (1) the local high PV value observed near ∼600 hPa is not a true stratospheric characterized intrusion but rather adiabatically produced high PV (e.g., Skerlak et al., 2015); (2) the relatively poor vertical resolution of AIRS ozone data may have limited the refined observation of the intrusions. From this figure, however, it is clear that stratospheric air (dry ozone-rich and high PV) intrusions have indeed occurred and were observed (at least intruded downward into ∼500 hPa).
3.4 Trajectory model analysis
Figure 9 shows 30 h backward trajectories ending at the radar site at 18:00 UT 29 November (panel a) and at 18:00 UT 30 November (panel b). As expected, the air mass parcel is transported eastward horizontally before the occurrence of main downdrafts (Fig. 9a), whereas after the downdrafts, the trajectories clearly show downward intrusions originated from the western site of Lake Baikal. Furthermore, a huge dry intrusion is tracked according to the criterion (based on a Lagrangian method) in Raveh-Rubin (2017). Trajectory results further support the evidence of downward intrusions that are closely related with the main downdrafts.
On the other hand, 30 h forward trajectories starting at 00:00 UT 30 November (panel a) and 00:00 UT 1 December (panel b) are shown in Fig. 10. It is interesting to note that, from Fig. 10a before the passage of COL, the air parcels at 4 km are transported rapidly upward (by more than 4 km within ∼23 h) and northeastward to the upper troposphere of eastern Siberia. This upward and poleward transport is associated with a warm conveyor belt (southerly flows dominate) that is located ahead of the COL. It contributes to the transport of the tropospheric moist and polluted air (such as aerosol) into the upper troposphere and even the lower stratosphere (e.g., Stohl et al., 2003; Sandhya et al., 2015). After the downdrafts, forward trajectories in Fig. 10b demonstrate that the dry intrusion air parcels continue to be transported downward and southeastward to the boundary layer or even the surface.
3.5 Strong downdrafts preceding rapid tropopause ascent – discussion
Figure 11a shows another 20 typical cases of strong downdrafts preceding rapid RT ascent for the period March 2012 and January 2015 (shown placed end to end); the LRT height (plotted by crosses) and the vertical velocity of the RT (plotted in orange line) are also plotted. These cases (marked by black rectangular boxes and labeled as S1, S2, S3, …, and S20) are identified based on the following criteria: (1) the amplitude of the RT ascent should exceed 0.6 km (four range gates), (2) vertical velocities of the RT ascent exceed 0.1 km h−1, (3) the downdrafts that occurred preceding the RT ascent should be > 0.5 m s−1, (4) the height region of the downdrafts should pass through the RT layer. The criteria are put forward mainly to avoid the influence of the RT spikes. Figure 11b shows the backward trajectories for the nine selected cases. Results show clear evidence of downward intrusions corresponding to the associated strong downdrafts. Their sources are mainly from western Siberia (western site of Lake Baikal), except for the Tr5 case. Moreover, according to AIRS daily 500 hPa ozone distribution, most of the cases in Fig. 11a (except for the cases S14, S15, S16, S17, S20) were associated with significant ozone enhancement, indicating intrusions of stratospheric origin (as shown in the Supplement Fig. S1). It is important to note that the RT excursion velocity values of the cases are not all above 0.2 km h−1, and some are lower than this value (e.g., cases S16 and S18). However, some form of stratospheric intrusions was exactly observed in such cases from both the trajectory and satellite results. Therefore, the threshold of vertical velocity of the RT ascent is set at 0.1 km h−1, rather than 0.2 km h−1 (Hocking et al., 2007). Large differences between RT and LRT are also interesting to note on some occasions when the RT changes rapidly (such as the occasion near 14 March 2012).
According to the meteorological chart, the synoptic situation of those cases identified in Fig. 11a is introduced. The cases S1, S2, S8, S9, S10, and S11 seem to have a close relationship with COL development; cases S3, S4, S5, S6, S7, S17, S18, and S19 seem to be associated with low or high trough systems (at 500 hPa). The remaining cases do not seem to be associated with any significant synoptic development. However, in terms of the distribution of isentropic PV (generally at 315 K in winter and 330 K in summer), we found that the remaining cases S12, S13, S14, S15, S16, and S20 appear to be associated with some form of stratospheric streamers and their breakup within the previous 48 h (not shown). Some cases (e.g., S1 and S2) that appear close on the same day were probably caused by the same system. The characteristics of the 20 cases, including the background synoptic condition, vertical velocity of the RT ascent, and 500 hPa ozone enhancement, have been summarized in Table 2.
In the light of the present understanding, the strong downdrafts preceding the rapid RT ascent can serve as an important diagnostic for intrusion events, during various synoptic processes in any season. This characteristic will be of great use and play an important role in routine identification of stratospheric intrusions. Considering the duration of such downdrafts, a higher time resolution of radar observations will be more helpful. The present study has shown that the duration of most downdrafts is generally within 1.5–3 h. We consider, therefore, that the radar resolution should be best within 1h.
Hocking et al. (2007) have reported that the rapid tropopause ascent (> 0.2 km h−1) alone can be a useful diagnostic for potential intrusion events. However, using only the information of RT heights might lead to non-negligible errors, as mentioned above in the Introduction, and according to the observations in Fig. 11. Especially on occasions when the RT ascent is between 0.1 and 0.2 km h−1 but the corresponding true intrusions were observed, all such intrusion events will be neglected (maybe ∼ two per month; refer to Fig. 12a), whereas on some occasions when the RT ascent exceeds 0.2 km h−1, but without observing true intrusion events (e.g., He et al., 2011), these events will be misdiagnosed (maybe ∼13 per month; refer to Fig. 12b). In this sense, using the unique MST radar observations of both the RT height variability and the vertical wind as a complementary signature for identifying possible intrusion events is very meaningful.
Figure 12 shows four years (2012–2015) of the events with rapid RT ascent (gray bands) and the events with strong downdrafts just preceding the rapid RT ascent (black bands). The identification criteria of such strong downdrafts are similar to that mentioned above and the events are classified according to different values of vertical velocity of the ascent. Among all the events with ascent velocity between 0.1 and 0.2 km h−1, about one-quarter (approximately two per month; Fig. 12a) were observed with strong downdrafts preceding them, whereas for the events with the ascent velocity > 0.2 km h−1, the proportion is about a half (approximately 10 per month; Fig. 12b). Here, according to the results above, the occurrence of the strong downdrafts just preceding the rapid RT ascent (black bands in Fig. 12) represents the occurrence of possible intrusions to a large degree. In this way, Fig. 12 indicates that the occurrence of possible intrusions exhibits distinct seasonal variations, with a maximum in winter and spring and a minimum in summer. This is because the mesoscale and small-scale atmospheric processes, such as cold air outbreaks, thunderstorms, and convective activities, are more active in winter and spring. They are important sources for downward stratospheric intrusions.
Detailed case analysis of the cross-tropopause stratospheric intrusions was carried out during a COL. Global reanalysis, satellite data, and HYSPLIT trajectories all showed consistent evidence of dry ozone-rich, high PV, and depleted CH4 air that penetrated downward into the free troposphere. The key signature of the stratospheric intrusions in the Beijing MST radar observations is the strong downdrafts just preceding the rapid RT ascent. The radar echo power decreased rapidly within the region of strong downdrafts, after which abnormal high aspect sensitivity was recorded in the troposphere. Such high aspect sensitivity served as another potential clue for the intrusions of stratospheric origin.
Based on the criteria mentioned in Sect. 3.5, 20 other typical cases of strong downdrafts preceding the rapid RT ascent between March 2012 and January 2015 were presented. These events occurred during different synoptic processes in different seasons. However, most of the cases (15 of them) are associated with some form of intrusions observed by a combination of AIRS-retrieved ozone and the HYSPLIT trajectory model. Our results show that the radar-derived tropopause height and vertical winds are strong complementary indicators to be used to infer the occurrence of the intrusions of stratospheric origin. This will be of great use and play an important role in the routine identification or prediction of intrusion events. However, the actual origin of the observed downdrafts preceding the rapid RT ascent is not addressed in this paper. Further combinations of observational experiments need to be conducted, especially using ozonesonde soundings, to quantitatively analyze the effectiveness of the present identification criteria for possible intrusions.
MST radar data are publicly and freely available at http://220.127.116.11/ (MST, 2018). AIRS data are publicly and freely available at https://disc.gsfc.nasa.gov/ (AIRS, 2018). ECMWF ERA-interim data are publicly and freely available at https://www.ecmwf.int/en/forecasts/datasets (ECMWF, 2018). Interpolated OLR data are available at https://www.esrl.noaa.gov/psd/ (OLR, 2018). Global radiosonde data publicly and freely available at http://weather.uwyo.edu/upperair/ (Radiosonde, 2018). HYSPLIT Trajectory model are publicly available at https://www.arl.noaa.gov/ (HYSPLIT, 2018).
The supplement related to this article is available online at: https://doi.org/10.5194/angeo-36-1403-2018-supplement.
GC, YT, SZ, and KH are the people in charge of MST radar data archiving, mage-generation and quality control. The HYSPLIT trajectory model analysis were performed by CS. The processing and data analysis for radar, satellite, and reanalysis data was developed by FC.
The authors declare that they have no conflict of interest.
The authors really appreciate Prof. Shira Raveh-Rubin for reading and
commenting the manuscript. This work is funded by the National Natural
Science Foundation of China (NSFC grants no. 41722404 and 41474132). The
authors would like to thank the staff of the Chinese Meridian Space Weather
Monitoring Project (CMSWMP) for their support in conducting the experiment.
The authors sincerely acknowledge the ECMWF, NASA, and NOAA Air Resources
Laboratory (ARL) for providing global reanalysis, satellite data, and the
HYSPLIT transport model, respectively. The interpolated OLR data are provided
by the NOAA/OAR/ESRL PSD, Boulder, Colorado, USA, from their website at
https://www.esrl.noaa.gov/psd/ (last access: 17 October 2018). The MST
radar data are available at the Data Centre for Meridian Space Weather
Monitoring Project (http://18.104.22.168/; last access: 17 October
2018). The radiosonde data are available from
http://weather.uwyo.edu/upperair/sounding.html (last access: 17 October
Edited by: Marc Salzmann
Reviewed by: two anonymous referees
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