Abstract
Through a cloud-resolving simulation of the rapid intensification (RI) of Typhoon Meranti (2016), the convections, warm core, and heating budget are investigated during the process of RI. By investigating the spatial distributions and temporal evolutions of both convective-stratiform precipitation and shallow-deep convections, we find that the inner-core convections take mode turns, from stratiform-precipitation (SP) dominance to convective-precipitation (CP) prevalence during the transition stages between pre-RI and RI. For the CP, it experiences fewer convections before RI, and the conversion from moderate/ moderate-deep convections to moderate-deep/deep convections during RI. There is a clear upper-level warm-core structure during the process of RI. However, the mid-low-level warming begins first, before the RI of Meranti. By calculating the local potential temperature (θ) budget of various convections, the link between convections and the warm core (and further to RI via the pressure drop due to the warming core) is established. Also, the transport pathways of heating toward the center of Meranti driven by pressure are illuminated. The total hydrostatic pressure decline is determined by the mid-low-level warm anomaly before RI, mostly caused by SP. The azimuthal-mean diabatic heating is the largest heating source, the mean vertical heat advection controls the vertical downwards transport by adiabatic warming of compensating down-drafts above eye region, and then the radial θ advection term radially transports heat toward the center of Meranti in a slantwise direction. Accompanying the onset of RI, the heating efficiency of the upper-level warming core rises swiftly and overruns that of the mid-low-level warm anomaly, dominating the total pressure decrease and being mainly led by moderate-deep and deep convections. Aside from the characteristics in common with SP, for CP, the eddy component of radial advection also plays a positive role in warming the core, which enhances the centripetal transport effect and accelerates the RI of Meranti.
Similar content being viewed by others
References
Chen H, Zhang D L (2013). On the rapid intensification of Hurricane Wilma (2005). Part II: convective bursts and the upper-level warm core. J Atmos Sci, 70(1): 146–162
Chen X M, Xue M, Fang J (2018). Rapid intensification of Typhoon Mujigae (2015) under different sea surface temperatures: structural changes leading to rapid intensification. J Atmos Sci, 75(12): 4313–4335
CMA (2016). Member Report: China. ESCAP/WMO Typhoon Committee: 9–14
DeMaria M, Sampson C R, Knaff J A, Musgrave K D (2014). Is tropical cyclone intensity guidance improving? Bull Am Meteorol Soc, 95(3): 387–398
Guimond S R, Heymsfield G M, Turk F J (2010). Multiscale observations of hurricane Dennis (2005): the effects of hot towers on rapid intensification. J Atmos Sci, 67(3): 633–654
Han B, Fan J, Varble A, Morrison H, Williams C R, Chen B, Dong X, Giangrande S E, Khain A, Mansell E, Milbrandt J A, Shpund J, Thompson G (2019). Cloud-resolving model intercomparison of an MC3E squall line case. Part II: stratiform precipitation properties. J Geophys Res D Atmospheres, 124(2): 1090–1117
Hendricks D A, Peng M S, Fu B, Li T (2010). Quantifying environmental control on tropical cyclone intensity change. Mon Weather Rev, 138(8): 3243–3271
Heymsfield G M, Halverson J B, Simpson J, Tian L, Bui T P (2001). ER-2 Doppler radar investigations of the eyewall of Hurricane Bonnie during the convection and moisture Experiment-3. J Appl Meteorol, 40(8): 1310–1330
Hirschberg P A, Fritsch J M (1993). On understanding height tendency. Mon Weather Rev, 121(9): 2646–2661
Huang Y, Wang Y, Cui X (2019). Differences between convective and dtratiform precipitation budgets in a torrential rainfall event. Adv Atmos Sci, 36(5): 495–509
Kaplan J, DeMaria M (2003). Large-scale characteristics of rapidly intensifying tropical cyclones in the North Atlantic basin. Weather Forecast, 18(6): 1093–1108
Li M X, Ping F, Tang X B, Yang S (2019). Effects of microphysical processes on the rapid intensification of Super-Typhoon Meranti. Atmos Res, 219: 77–94
Li Q Q, Wang Y Q (2012). A comparison of inner and outer spiral rainbands in a numerically simulated tropical cyclone. Mon Weather Rev, 140(9): 2782–2805
Lin I I, Wu C C, Pun I F, Ko D S (2008). Upper-ocean thermal structure and the western North Pacific category 5 typhoons. Part I: ocean features and the category 5 typhoons’ intensification. Mon Weather Rev, 136(9): 3288–3306
Marks F D, Shay L K (1998). Landfalling tropical cyclones: forecast problems and associated research opportunities. Bull Am Meteorol Soc, 79(2): 305–323
Molinari J, Vollaro D (2010). Rapid intensification of a sheared tropical storm. Mon Weather Rev, 138(10): 3869–3885
Nguyen L T, Molinari J (2012). Rapid intensification of a sheared, fast-moving hurricane over the Gulf Stream. Mon Weather Rev, 140(10): 3361–3378
Reasor P D, Eastin M D, Gamache J F (2009). Rapidly intensifying Hurricane Guillermo (1997). Part I: low-wavenumber structure and evolution. Mon Weather Rev, 137(2): 603–631
Rogers R (2010). Convective-scale structure and evolution during a high-resolution simulation of tropical cyclone rapid intensification. J Atmos Sci, 67(1): 44–70
Rogers R F, Reasor P D, Zhang J A (2015). Multiscale structure and evolution of Hurricane Earl (2010) during rapid intensification. Mon Weather Rev, 143(2): 536–562
Steiner M, Houze R A Jr, Yuter S E (1995). Climatological characterization of three-dimensional storm structure from operational radar and rain gauge data. J Appl Meteorol, 34(9): 1978–2007
Stern D P, Zhang F Q (2013). How does the eye warm? Part I: a potential temperature budget analysis of an idealized tropical cyclone. J Atmos Sci, 70(1): 73–90
Sun Y Q, Jiang Y X, Tan B, Zhang F Q (2013). The governing dynamics of the secondary eyewall formation of Typhoon Sinlaku (2008). J Atmos Sci, 70(12): 3818–3837
Tao C, Jiang H (2015). Distributions of shallow to very deep precipitation-convection in rapidly intensifying tropical cyclones. J Clim, 28(22): 8791–8824
Wang H, Wang Y Q (2014). Full access a numerical study of Typhoon Megi (2010). Part I: rapid intensification. Mon Weather Rev, 142(1): 29–48
Wang Y Q (2009). How do outer spiral rainbands affect tropical cyclone structure and intensity? J Atmos Sci, 66(5): 1250–1273
Wang Y, Wu C C (2004). Current understanding of tropical cyclone structure and intensity changes—a review. Meteor Atmos Phys, 87 6(4): 257–278
Zhang D L, Chen H (2012). Importance of the upper-level warm core in the rapid intensification of a tropical cyclone. Geophys Res Lett, 39 (2): L02806
Zheng Y, Gong Y, Chen J, Tian F (2019). Warm-season diurnal variations of total, stratiform, convective, and extreme hourly precipitation over central and eastern China. Adv Atmos Sci, 36(2): 143–159
Acknowledgements
Very thanks for the valuable comments of the three anonymous reviewers, which helped considerably in improving the original manuscript. This work was supported by the National Key Research and Development Program of China (Grant Nos. 2018YFC1506801 and 2018YFF0300102), the Plateau Atmosphere and Environment Key Laboratory of Sichuan Province (Grant No. PAEKL-2017-K3), and the National Natural Science Foundation of China (Grant Nos. 41405059, 41575064, 41875079, 41875077, 41575093, and 41630532).
Author information
Authors and Affiliations
Corresponding authors
Rights and permissions
About this article
Cite this article
Tang, X., Ping, F., Yang, S. et al. On the rapid intensification for Typhoon Meranti (2016): convection, warm core, and heating budget. Front. Earth Sci. 13, 791–807 (2019). https://doi.org/10.1007/s11707-019-0799-z
Received:
Accepted:
Published:
Issue Date:
DOI: https://doi.org/10.1007/s11707-019-0799-z