Please wait a minute...
Frontiers of Earth Science

ISSN 2095-0195

ISSN 2095-0209(Online)

CN 11-5982/P

Postal Subscription Code 80-963

2018 Impact Factor: 1.205

Front. Earth Sci.    2019, Vol. 13 Issue (4) : 808-816    https://doi.org/10.1007/s11707-019-0792-6
RESEARCH ARTICLE
Large-scale characteristics of landfalling tropical cyclones with abrupt intensity change
Qianqian JI1,2, Feng XU1,2,3(), Jianjun XU1,2,3(), Mei LIANG1,2, Shifei, TU1,2, Siqi, CHEN1,2
1. South China Sea Institute of Marine Meteorology, Guangdong Ocean University, Zhanjiang 524088, China
2. College of Ocean and Meteorology, Guangdong Ocean University, Zhanjiang 524088, China
3. Southern Marine Science and Engineering Guangdong Laboratory, Zhanjiang 524088, China
 Download: PDF(1943 KB)   HTML
 Export: BibTeX | EndNote | Reference Manager | ProCite | RefWorks
Abstract

Data from the China Meteorological Administration and ERA-Interim are used to examine the environmental characteristics of landfalling tropical cyclones (TCs) with abrupt intensity change. The results show that, of all 657 landfalling TCs during 1979–2017, 71%, 70% and 65% of all landfalling TDs, TSs and TYs, respectively, intensify. Of all the 16595 samples, 4.0% and 0.2% of typhoons and tropical storms, respectively, experience over-water rapid intensification (RI) process during their life cycle. Meanwhile, 4.5% and 0.6% of typhoons and tropial storms, respectively, undergo over-water rapid decay (RD). These two kinds of cases, i.e., RI and RD, are used to analyze their associated large-scale conditions. Comparisons show that the RI cases are generally on the south side of the strong western Pacific subtropical high (WPSH); warm sea surface temperatures (SSTs) and sufficient water vapor fluxes existing in RI samples is a dominant feature that is conducive to the development of TCs. Also, the moderate low-level relative vorticity is favorable for TC intensification. On the contrary, the RD TCs are located on the west side of the WPSH; significant decreasing SSTs and low-level water vapor transport may synergistically contribute to RD. Simultaneously, low-level relative vorticity seems to be unfavorable for the development of TCs.

Keywords landfalling tropical cyclone      abrupt intensity change      environmental factors      dynamic composite analysis     
Corresponding Author(s): Feng XU,Jianjun XU   
Just Accepted Date: 16 October 2019   Online First Date: 26 November 2019    Issue Date: 30 December 2019
 Cite this article:   
Qianqian JI,Feng XU,Jianjun XU, et al. Large-scale characteristics of landfalling tropical cyclones with abrupt intensity change[J]. Front. Earth Sci., 2019, 13(4): 808-816.
 URL:  
https://academic.hep.com.cn/fesci/EN/10.1007/s11707-019-0792-6
https://academic.hep.com.cn/fesci/EN/Y2019/V13/I4/808
Fig.1  Frequency distribution of the DV24 in each TC grade.
Intensity class N Mean
/(m·s-1)
Std
dev
/(m·s-1)
Min
/(m·s-1)
Max
/(m·s-1)
TD 831 - 0.12 2.5 - 12 15
TS 4661 0.37 5.49 - 25 16
TY 11103 0.48 9.87 - 47 45
All TCs 16595 0.41 8.6 - 47 45
Tab.1  The DV24 statistics of TDs, TSs, TYs, and all TC intensity classes. The number of cases (N), mean, standard deviation (std dev), minimum (min), and maximum (max) DV24 are also provided
Class No. and name Time Position Pressure /hPa Wind speed /(m·s-1) DV24/(m·s-1)
RI 8521 (Dot) 1985/10/14/00 (11.6°N, 142.3°E) 992 20 15
8807 (Bill) 1988/08/06/06 (25.0°N, 128.0°E) 998 15 15
9025 (Mike) 1990/11/10/00 (8.6°N, 135.9°E) 960 40 20
0518 (Damrcy) 2005/09/24/06 (19.7°N, 114.8°E) 980 30 20
0621 (Chebi) 2006/11/09/06 (15.9°N, 131.3°E) 1000 15 30
1319 (Usagi) 2013/09/17/18 (17.2°N, 130.7°E) 990 23 15
1601 (Mujigae) 2016/07/04/06 (12.8°N, 141.0°E) 992 23 17
RD 7908 (Hope) 1979/08/01/06 (20.9°N, 121.7°E) 910 60 -15
8504 (Hal) 1985/06/23/06 (21.4°N, 117.1°E) 965 40 -15
9003 (Marian) 1990/05/18/00 (18.9°N, 114.3°E) 965 40 - 20
9521 (Kent) 1995/11/01/18 (14.4°N, 126.8°E) 925 60 -20
0713 (Wipha) 2007/09/18/00 (24.4°N, 123.6°E) 935 55 - 25
0815 (Jangmi) 2008/09/27/12 (21.3°N, 124.4°E) 910 65 -20
1614 (Meranti) 2016/09/13/12 (20.4°N, 122.9°E) 890 75 -20
Tab.2  List of basic conditions at the beginning of the 24 h periods of selected samples
Fig.2  The 500-hPa geopotential height (solid line) and wind vector (arrows) field of RI and RD TCs (a) at the beginning of RI; (b) at the end of RI; (c) at the beginning of RD; and (d) at the end of RD (units: dagpm). The origin of the coordinates is the TC center; the north and east direction are positive and the south and west are negative.
Fig.3  The 850-hPa wind and water vapor fluxes of the RI and RD TCs (a) at the beginning of RI, (b) at the end of RI, (c) at the beginning of RD, and (d) at the end of RD (units: g/(s?hPa?cm)).
Fig.4  Vertical wind shear of RI and RD TCs (a) at the beginning of RI; (b) at the end of RI; (c) difference between the beginning and end of RI; (d) at the beginning of RD; (e) at the end of RD; and (f) difference between the beginning and end of RD (units: m/s).
Fig.5  Relative vorticity (contours; units: × 10-6 /s) and divergence (shaded; red:≥1.5 × 10-6 /s, gray:≤- 1.5 × 10-6 /s) latitudinal-vertical profile of RI and RD TCs (a) at the beginning of RI; (b) at the end of RI; (c) difference between the beginning and end of RI; (d) at the beginning of RD; (e) at the end of RD; and (f) difference between the beginning and end of RD (units: /s).
Variable RI RD D=
RD- RI
beginning differences beginning differences
SST / °C 29.03 -0.37 28.19 -0.78* -0.84*
Water vapor fluxes / (g / (s?hPa?cm)-1) 23.38 1.43 15.88 -0.63 -7.50*
vertical wind shear / (m·s-1) 0.51 0.39 0.53 0.98 0.02
850 hPa relative vorticity / (10-6·s-1) 25.31 0.38 34.93 -1.95 9.62
Tab.3  The mean values of synoptic variables at the initial (t = 0) time and average differences between end and beginning of the RI and RD samples. The differences between these mean values (D= RD- RI) are also shown. The algorithm is applied within 550 km of the TC center. An asterisk indicates statistical significance at the 95% confidence level
1 L F Bosart, C S Velden, W E Bracken, J Molinari, P G Black (2000). Environmental influences on the rapid intensification of Hurricane Opal (1995) over the Gulf of Mexico. Mon Weather Rev, 128(2): 322–352
https://doi.org/10.1175/1520-0493(2000)128<0322:EIOTRI>2.0.CO;2
2 J C L Chan, Y Duan, L K Shay (2001). Tropical cyclone intensity change from a simple ocean-atmosphere coupled model. J Atmos Sci, 58(2): 154–172
https://doi.org/10.1175/1520-0469(2001)058<0154:TCICFA>2.0.CO;2
3 M DeMaria (1996). The effect of vertical wind shear on tropical cyclone intensification change. J Atmos Sci, 53: 2076–2088
https://doi.org/10.1175/1520-0469(1996)053%3C2076:TEOVSO%3E2.0.CO;2
4 R L Elsberry, T D B Lambert, M A Boothe (2007). Accuracy of Atlantic and eastern North Pacific tropical cyclone intensity forecast guidance. Weather Forecast, 22(4): 747–762
https://doi.org/10.1175/WAF1015.1
5 R L Elsberry (2014). Advances in research and forecasting of tropical cyclones from 1963–2013. Asia-Pacc J Atmos Sci, 50(1): 3–16
https://doi.org/10.1007/s13143-014-0001-1
6 K A Emanuel (1999). Thermodynamic control of hurricane intensity. Nature, 401(6754): 665–669
https://doi.org/10.1038/44326
7 K Emanuel, C DesAutels, C Holloway, R Korty (2004). Environmental control of tropical cyclone intensity. J Atmos Sci, 61(7): 843–858
https://doi.org/10.1175/1520-0469(2004)061<0843:ECOTCI>2.0.CO;2
8 W M Gray, L R Brody (1967). Global view of the origin of tropical disturbances and storms. Atmospheric Sci Pape, 114
https://doi.org/10.1.1.848.9817&rep=rep1&type=pdf
9 W Huang, X Liang (2010). Convective asymmetries associated with tropical cyclone landfall; β-plane simulations. Adv Atmos Sci, 27(4): 795–806
https://doi.org/10.1007/s00376-009-9086-3
10 H Jiang (2012). The relationship between tropical cyclone intensity change and the strength of inner-core convection. Mon Weather Rev, 140(4): 1164–1176
https://doi.org/10.1175/MWR-D-11-00134.1
11 J Kaplan, M DeMaria (2003). Large-scale characteristics of rapidly intensifying tropical cyclones in the North Atlantic basin. Weather Forecast, 18(6): 1093–1108
https://doi.org/10.1175/1520-0434(2003)018<1093:LCORIT>2.0.CO;2
12 J Kaplan, M DeMaria, J A Knaff (2010). A revised tropical cyclone rapid intensification index for the Atlantic and eastern North Pacific basins. Weather Forecast, 25(1): 220–241
https://doi.org/10.1175/2009WAF2222280.1
13 J Liang, L Wu, G Gu (2018). Rapid weakening of tropical cyclones in monsoon gyres over the tropical western North Pacific. J Clim, 31(3): 1015–1028
https://doi.org/10.1175/JCLI-D-16-0784.1
14 I I Lin, C C Wu, K Emanuel, I H Lee, C R Wu, I F Pun (2005). The interaction of Super Typhoon Maemi (2003) with a warm ocean eddy. Mon Weather Rev, 133(9): 2635–2649
https://doi.org/10.1175/MWR3005.1
15 A Lowag, M L Black, M D Eastin (2008). Structural and intensity change of Hurricane Bret (1999). Part I: environmental influences. Mon Weather Rev, 136(11): 4320–4333
https://doi.org/10.1175/2008MWR2438.1
16 R T Merrill (1988). Environmental influences on hurricane intensification. J Atmos Sci, 45(11): 1678–1687
https://doi.org/10.1175/1520 0469(1988)045<1678:EIOHI>2.0.CO;2
17 L A Paterson, B N Hanstrum, N E Davidson, H C Weber (2005). Influence of environmental vertical wind shear on the intensity of hurricane-strength tropical cyclones in the Australian region. Mon Weather Rev, 133(12): 3644–3660
https://doi.org/10.1175/MWR3041.1
18 R L Pfeffer, M Challa (1981). A numerical study of the role of eddy fluxes of momentum in the development of Atlantic hurricanes. J Atmos Sci, 38(11): 2393–2398
https://doi.org/10.1175/1520-0469(1981)038<2393:ANSOTR>2.0.CO;2
19 I F Pun, Y T Chang, I I Lin, T Y Tang, R C Lien (2011). Typhoon-ocean interaction in the Western North Pacific, Part 2. Oceanography (Wash DC), 24(4): 32–41
https://doi.org/10.5670/oceanog.2011.92
20 R W Reynolds, T M Smith, C Liu, D B Chelton, K S Casey, M G Schlax (2007). Daily high-resolution-blended analyses for sea surface temperature. J Clim, 20(22): 5473–5496
https://doi.org/10.1175/2007JCLI1824.1
21 S Shu, J Ming, P Chi (2012). Large-scale characteristics and probability of rapidly intensifying tropical cyclones in the western North Pacific basin. Weather Forecast, 27(2): 411–423
https://doi.org/10.1175/WAF-D-11-00042.1
22 A Simmons (2006). ERA-Interim: new ECMWF reanalysis products from 1989 onwards. ECMWF Newsletter, 110: 25–36
23 H E Willoughby, J A Clos, M G Shoreibah (1982). Concentric eye walls, secondary wind maxima, and the evolution of the hurricane vortex. J Atmos Sci, 39(2): 395–411
https://doi.org/10.1175/1520-0469(1982)039<0395:CEWSWM>2.0.CO;2
24 K M Wood, E A Ritchie (2015). A definition for rapid weakening of North Atlantic and eastern North Pacific tropical cyclones. Geophys Res Lett, 42(22): 10–091
https://doi.org/10.1002/2015GL066697
25 T Yuan, H Jiang (2010). Forecasting rapid intensification of tropical cyclones in the western North Pacific using TRMM/TMI 37 GHz microwave signal. In: 65th Interdepartmental Hurricane Conference (IHC). Miami, USA
26 Q Zhang, L Wu, Q Liu (2009). Tropical cyclone damages in China 1983–2006. Bull Am Meteorol Soc, 90(4): 489–496
https://doi.org/10.1175/2008BAMS2631.1
[1] FES-19792-OF-JQQ_suppl_1 Download
Viewed
Full text


Abstract

Cited

  Shared   
  Discussed