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Diurnal Variation of the Convective Area and Eye Size Associated with the Rapid Intensification of Tropical Cyclones

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Diurnal Variation of the Convective Area and Eye Size Associated with the Rapid Intensification of Tropical Cyclones OCTOBER 2020 L E E E T A L . 4061 Diurnal Variation of the Convective Area and Eye Size Associated with the Rapid Intensification of Tropical Cyclones JAE-DEOK LEE Department of Atmospheric Sciences, National Taiwan University, Taipei, Taiwan, and Department of Physics and Earth Sciences, University of the Ryukyus, Okinawa, Japan CHUN-CHIEH WU Department of Atmospheric Sciences, National Taiwan University, Taipei, Taiwan KOSUKE ITO Department of Physics and Earth Sciences, University of the Ryukyus, Okinawa, Japan (Manuscript received 15 October 2019, in final form 27 July 2020) ABSTRACT This study examines the diurnal variation of the convective area and eye size of 30 rapidly intensifying tropical cyclones (RI TCs) that occurred in the western North Pacific from 2015 to 2017 utilizing Himawari-8 satellite imagery. The convective area can be divided into the active convective area (ACA), mixed phase, and inactive convective area (IACA) based on specific thresholds of brightness temperature. In general, ACA tends to develop vigorously from late afternoon to early the next morning, while mixed phase and IACA develop during the day. This diurnal pattern indicates the potential for ACA to evolve into mixed phase or IACA over time. From the 30 samples, RI TCs tend to have at least a single-completed diurnal signal of ACA inside the radius of maximum wind (RMW) during the rapidly intensifying period. In the same period, the RMW also contracts significantly. Meanwhile, more intense storms such as those of category 4 or 5 hurricane intensity are apt to have continuous ACA inside the RMW and maintain eyewall convective clouds. These diurnal patterns of the ACA could vary depending on the impact of large-scale environments such as vertical wind shear, ocean heat content, environmental mesoscale convection, and terrain. The linear regression analysis shows that from the tropical storm stage, RI commences after a slow intensification period, which enhances both the primary circulation and eyewall convective cloud. Finally, after the eye structure appears in satellite imagery, its size changes inversely to the diurnal variation of the convective activity (e.g., the eye size becomes larger during the daytime). KEYWORDS: Diurnal effects; Tropical cyclones; Satellite observations 1. Introduction Jiang 2012; Kieper and Jiang 2012; Monette et al. 2012). In general, since the IR window channel around 11 mm Satellite imagery can provide massive amounts of in- is not significantly absorbed by atmospheric gases, formation over extensive areas, and multiple previous it has been widely used to monitor convective or studies have used infrared (IR) brightness temperature stratiform clouds. Previous studies have shown that to examine convective clouds related to tropical cy- cold brightness temperature suitable for indicating the clones (TCs) (Browner et al. 1977; Muramatsu 1983; convective area could be used as one of the indicators Steranka et al. 1986; Harnos and Nesbitt 2011, 2016; of TC intensification (Gentry et al. 1980; Jiang 2012; Monette et al. 2012; Fischer et al. 2018). For example, Supplemental information related to this paper is available Gentry et al. (1980) demonstrated that a future (124 h) at the Journals Online website: https://doi.org/10.1175/MWR-D- TC intensity change is strongly correlated with the 19-0345.s1. mean brightness temperature at a correlation coeffi- cient of 20.781. This relationship was also similarly Corresponding author: Dr. Chun-Chieh Wu, [email protected] confirmed by Monette et al. (2012) using a tropical DOI: 10.1175/MWR-D-19-0345.1 Ó 2020 American Meteorological Society. For information regarding reuse of this content and general copyright information, consult the AMS Copyright Policy (www.ametsoc.org/PUBSReuseLicenses). Unauthenticated | Downloaded 10/07/21 11:25 AM UTC 4062 MONTHLY WEATHER REVIEW VOLUME 148 overshooting tops algorithm for rapid intensification environment, TC frequently fails to intensify due to (RI) prediction. significant precession motion or decoupling between the In total, 85 GHz microwave satellite imagery may lower troposphere circulation and the upper-troposphere have an advantage in detecting deep convective cells circulation, but the above mechanism is not as clear for 2 related to ice scattering (Jiang 2012; Fischer et al. 2018), moderate VWS (5–10 m s 1). and these deep convective cells may release abundant Meanwhile, deep convective cells are recognized as a latent heat above the freezing level. Jiang (2012) dem- primary source of the cirrus shield, which is also referred onstrated that RI TCs have the lowest 11-mm brightness to as the central dense overcast or cirrus canopy in the temperature ranging from 174 to 223 K and the tallest upper troposphere (Malkus et al. 1961; Sadler 1964; 20-dBZ echo height compared to other TC phases such Merritt and Wexler 1967; Weickmann et al. 1977; Gray as slow intensification (SI), weakening (W), and neutral and Jacobson 1977; Dunion et al. 2014). According to (N). Fischer et al. (2018) also showed that TCs in the RI Merritt and Wexler (1967), the maximum areal extent of stage exhibit more concentrated cold brightness tem- these cirrus clouds appears 12 to 18 h after deep con- peratures inside the 100-km radius than in other stages. vection initiation, that is, the cirrus cloud coverage is out These results support the statement that convective of phase approximately 12 h from the diurnal signal of bursts (CBs) can contribute to TC intensification by convective clouds (Browner et al. 1977; Muramatsu releasing substantial latent heat, as much as 6.6 3 1017 J 1983; Steranka et al. 1984; Kossin 2002; Dunion et al. in a 12-h period inside the inner-core area (Kelley and 2014; Leppert and Cecil 2016). Browner et al. (1977) Halverson 2011). This additional latent heat may in- discussed that the maximum 253-K area decreases as TC crease TC intensity at a rate that satisfies the general RI intensity increases. For example, the average magnitude threshold of Kaplan and DeMaria (2003) in a 24-h pe- of the diurnal oscillation in the area of the cloud canopy riod. The increase in convective cells can also contribute computed by comparing the maximum area with the to a significant contraction of the radius of maximum minimum area in the tropical depression and hurricane wind (RMW) through radially varying diabatic heating is 3.03 and 2.09, respectively. This result indicates that (Schubert and Hack 1982; Willoughby 1990). This con- the diurnal area oscillation appears to be more signifi- tracted RMW could be an efficient configuration for TC cant in tropical depressions than in hurricanes. spinup by concentrating diabatic heating in the high- Gray and Jacobson (1977) showed that the upper inertial stability area, e.g., inside the RMW excluding disturbance area could experience a significant net ra- the eye region (Vigh and Schubert 2009). diational warming and cooling for one day. However, in RI is primarily initiated at the tropical storm and the disturbance area, e.g., thick cloud area, the tem- category 1 hurricane intensity stage (Kaplan and DeMaria perature remains warm in the midtroposphere and 2003; Hendricks et al. 2010; Jiang 2012). Previous studies lower troposphere despite temperature changes induced have shown that right before the onset of RI, CBs are by the net radiation. It may be due to longwave emission- frequently observed near the RMW and also in downshear reabsorption and condensate heat from the vapor. It may quadrants (Braun et al. 2006; Braun and Wu 2007; Reasor be due to longwave emission-reabsorption and condensate et al. 2009; Rogers 2010; Guimond et al. 2010, 2016; Rogers heat from the vapor. Therefore, the net radiational con- et al. 2013, 2015; DeHart et al. 2014; Chang and Wu 2017; trast between daytime and nighttime may significantly Hazelton et al. 2017a,b; Fischer et al. 2018; Lee and Wu contribute to the stability between the upper and lower 2018). However, these deep convective cells could be clouds. Navarro and Hakim (2016) showed contrasting suppressed and tilted outward in upshear quadrants as a daytime and nighttime vertical flow patterns (see their result of significant convective-scale subsidence or the Figs. 8 and 9). Specifically, the vertical circulation related vertical wind shear (VWS) (Chen and Gopalakrishnan to the net radiative tendency appears as cyclonic circula- 2015; Lee and Wu 2018). In the moderate or strong VWS tion in the afternoon and changes into anticyclonic circu- environments, the vortex structure is typically tilted lation in the early morning, which could explain certain according to the VWS direction, but intensifying TCs physical mechanisms concerning the convective activity could overcome such tilted structure as a result of suf- invigorated between late afternoon and midnight. Tang ficient inner-core convective cells that serve to reduce et al. (2019) discussed that the diurnal radiation contrast the precession motion of the vortex (Gray 1968; Jones was significant for changes in the RMW. For example, 1995; DeMaria 1996; Frank and Ritchie 1999, 2001; the RMW contraction tends to be more accelerated Reasor et al. 2004; Braun and Wu 2007; Rios-Berrios et al. during the nighttime due to the radiative destabilization 2018; Lee and Wu 2018). These processes in sequence and moistening in the lower troposphere compared to may be how a TC reintensifies in a moderate or strong the daytime. Muramatsu (1983) discussed the diurnal 2 VWS environment. Under a strong VWS (.10 m s 1) variation of the maximum extent of convective clouds Unauthenticated | Downloaded 10/07/21 11:25 AM UTC OCTOBER 2020 L E E E T A L . 4063 and the eye diameter in mature TCs and stated that the channels between 10 and 12 mm are not significantly convective area corresponding to a 2708C brightness absorbed by atmospheric gases, these wavelengths have temperature could reach its maximum size between been widely used to monitor severe weather systems the afternoon-evening and early morning, whereas the like supercells or intensifying TCs.
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