Effect of convection on the thermal structure of the troposphere and lower stratosphere including the tropical tropopause layer in the South Asian monsoon region

Muhsin, M.; Sunilkumar, S. V.; Ratnam, M. Venkat; Parameswaran, K.; Murthy, B. V. Krishna; Emmanuel, Maria

doi:10.1016/j.jastp.2018.01.016

Cited by 13 publications

(10 citation statements)

References 40 publications

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“…At an altitude of about 14 km, the temperature profiles of the convective overshooting and the mean temperature profiles become similar. From 14-to 18-km altitude, cooling temperature anomalies during convective overshooting are found, and the biggest anomalies (23.5 K for COSMIC; 24.1 K for ERA5; 23.8 K for JRA-55; 24 K for MERRA-2; 23 K for IGRA) appear at about 15-17-km altitude, which is consistent with previous study (Chae et al 2011;Kim et al 2018;Muhsin et al 2018;Johnston et al 2018). In the lower stratosphere (;17-10 km), the cooling anomalies caused by convective overshooting are obviously lower than that by normal convective based on the results from ERA5, JRA-55, and MERRA-2.…”

Section: Temperature Profiles Of the Convective Overshootingsupporting

confidence: 92%

“…In the lower stratosphere (;17-10 km), the cooling anomalies caused by convective overshooting are obviously lower than that by normal convective based on the results from ERA5, JRA-55, and MERRA-2. Moreover, warming anomalies appear in the lower stratosphere calculated by COSMIC and the biggest warming anomalies can reach to 1.2 K. Muhsin et al (2018) also find deep convection warm the lower stratosphere (17.5 km), with a sharp peak (;3 K). Near the tropopause (16 6 2 km), the difference between the temperature profiles of the convection and the mean temperature is lower than that between the temperature profiles of the convective overshooting and the mean temperature.…”

Section: Temperature Profiles Of the Convective Overshootingmentioning

confidence: 64%

“…Xian and Fu (2015) find that the updraft within convective overshooting can partly account for the warm anomalies in the upper troposphere by calculating the convectively available potential energy. Gettelman and Birner (2007) show that the latent heat release in and near convective clouds leads to the warm anomalies throughout the middle troposphere, which is widely accepted (Muhsin et al 2018;Johnston et al 2018).…”

Section: E Discussion Of the Physical Process In Convective Overshootingmentioning

confidence: 94%

“…It has long been understood that convective overshooting strongly affects the thermal structure (Sherwood and Wahrlich 1999;Kuang and Bretherton 2004;Luo et al 2008;Mitovski et al 2010;Paulik and Birner 2012;Folkins 2013;Xian and Fu 2015), moisture distribution (Chae et al 2011;Kim et al 2018;Muhsin et al 2018), and chemical constituents (Thompson et al 1997;Yi et al 2012) of the troposphere and lower stratosphere. Fully understanding these important influences requires, in part, accurate methods of observing large-scale and long-term distribution and frequency of convective overshooting and obtaining temperature profiles with high vertical resolution and accuracy near tropopause altitudes during severe weather events.…”

Section: Introductionmentioning

confidence: 99%

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The impact of convective overshooting on the thermal structure over the Tibetan Plateau in summer based on TRMM, COSMIC, radiosonde and reanalysis data

Sun

Zhong

et al. 2021

Journal of Climate

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In this paper, we examine convective overshooting and its effects on the thermal structure of the troposphere and lower stratosphere in the Tibetan Plateau in summer by matching the Tropical Rainfall Measuring Mission (TRMM) with Integrated Global Radiosonde Archive (IGRA), Constellation Observing System for Meteorology, Ionosphere, and Climate (COSMIC), European Centre for Medium-Range Weather Forecasts 5th Reanalysis (ERA-5), the Japanese Meteorological Association 55-year reanalysis (JRA-55) and the National Aeronautics and Space Administration Modern-Era Retrospective analysis for Research and Applications, Versions2 (MERRA-2). It was found that convective overshooting mainly occurs in the central and eastern part of the Tibetan Plateau, and its frequency varies from 0.01 × 10−4 to 0.91 × 10−4. The convective overshooting warms the low middle tropopause and cools the tropopause nearby significantly, which can also makes air get wetter. The tropopause of the convective overshooting is substantially lower than the mean tropopause. Statistical results calculated from the five datasets are generally consistent; however, each dataset has its own strengths and weaknesses. The high spatiotemporal resolution temperature profiles from ERA-5 along with the high vertical resolution temperature profiles from COSMIC can be combined to accurately study convective overshooting in the Tibetan Plateau.

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Section: Temperature Profiles Of the Convective Overshootingsupporting

confidence: 92%

Section: Temperature Profiles Of the Convective Overshootingmentioning

confidence: 64%

Section: E Discussion Of the Physical Process In Convective Overshootingmentioning

confidence: 94%

Section: Introductionmentioning

confidence: 99%

See 2 more Smart Citations

The impact of convective overshooting on the thermal structure over the Tibetan Plateau in summer based on TRMM, COSMIC, radiosonde and reanalysis data

Sun

Zhong

et al. 2021

Journal of Climate

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“…Figure 1 shown) shows the persistence of waves in the UTLS region on this day. There were several studies showing the influence of deep convection and waves on the temperature and water vapour in the UTLS region (eg: Suzuki et al, 2013;Sunilkumar et al, 2016;Muhsin et al, 2018). This cooler tropopause might be responsible for the freeze drying around this region resulting in a sharp minimum in WVMR close to the CPT.…”

Section: Altitude Distribution Of Lower Stratospheric Water Vapour Anmentioning

confidence: 99%

Annual cycle of water vapour in the lower stratosphere over the Indian Peninsula derived from Cryogenic Frost-point Hygrometer observations

Emmanuel

Muhammed

Kumar

et al. 2018

Preprint

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Abstract. In situ measurements of lower stratospheric water vapour employing Cryogenic Frost point Hygrometer (CFH) over two tropical stations, Trivandrum (8.53&deg;N, 76.87&deg;E) and Hyderabad (17.47&deg;N, 78.58&deg;E) over the Indian subcontinent are conducted as part of Tropical Tropopause Dynamics (TTD) monthly campaigns under GARNETS program. The annual variation of lower stratosphere (LS) water vapour clearly depicts the so called tape recorder effect at both the stations. The ascent rate of water vapour compares well with the velocity of Brewer-Dobson circulation and is slightly higher over the equatorial station when compared to the off-equatorial station. The column integrated water vapour in the LS varies in the range 1.5 to 4g/m2 with low values during winter and high values during summer monsoon and post monsoon seasons and its variability shows the signatures of local dynamics. The variation in water vapour mixing ratio (WVMR) at the cold point tropopause (CPT) exactly follows the variation in CPT temperature. The difference in WVMR between the stations shows a semi-annual variability in the altitude region 18&ndash;20km region with high values of WVMR during summer monsoon and winter over Hyderabad and during pre-monsoon and post-monsoon over Trivandrum. This difference is related to the influence of the variations in local CPT temperature and deep convection. The monsoon dynamics has a significant role in stratospheric water vapour distribution in summer monsoon season.

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Observational evidence of the relationship between the tropical tropopause and tropical easterly jet streams over the Indian monsoon region

Mehta

2024

Atmospheric Science Letters

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This paper presents the first quantitative relationship between the cold point tropopause (CPT) and tropical easterly jet (TEJ) using radiosonde observations over Gadanki (13.45° N, 79.2° E) during the Indian summer monsoon season 2006–2014. CPT and TEJ peak altitudes () show amalgams of two categories of variability on the day‐to‐day scale. In category1 occurs close to and they show in‐phase variation. While in Category2 occurs far apart from and they do not show any relationship. For Category1 and are strongly correlated (0.70), as well as and (CPT temperature) are moderately anticorrelated (−0.55) significant at a 95% confidence level, indicating the dominance of adiabatic processes. Whereas in Category2 and are not significantly anti‐correlated. Thus, when TEJ and CPT are close to each other, it may serve as an indicator for the prevalence of the synoptic‐scale effect.

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Effect of convection on the thermal structure of the troposphere and lower stratosphere including the tropical tropopause layer in the South Asian monsoon region

Cited by 13 publications

References 40 publications

The impact of convective overshooting on the thermal structure over the Tibetan Plateau in summer based on TRMM, COSMIC, radiosonde and reanalysis data

The impact of convective overshooting on the thermal structure over the Tibetan Plateau in summer based on TRMM, COSMIC, radiosonde and reanalysis data

Annual cycle of water vapour in the lower stratosphere over the Indian Peninsula derived from Cryogenic Frost-point Hygrometer observations

Observational evidence of the relationship between the tropical tropopause and tropical easterly jet streams over the Indian monsoon region

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