**Author details**

Song Yang\* and Joshua Cossuth

\*Address all correspondence to: song.yang@nrlmry.navy.mil

Naval Research Laboratory, Monterey, CA, USA

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#### **Satellite Climatology of Tropical Cyclone with Concentric Eyewalls Satellite Climatology of Tropical Cyclone with Concentric Eyewalls**

Yi-Ting Yang , Hung-Chi Kuo , Eric A. Hendricks and Melinda S. Peng Yi-Ting Yang, Hung-Chi Kuo, Eric A. Hendricks and Melinda S. Peng

Additional information is available at the end of the chapter

Additional information is available at the end of the chapter

http://dx.doi.org/10.5772/64354

#### **Abstract**

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170 Recent Developments in Tropical Cyclone Dynamics, Prediction, and Detection

An objective method is developed to identify concentric eyewalls (CEs) for tropical cyclones (TCs) using passive microwave satellite imagery from 1997 to 2014 in the western North Pacific (WNP) and Atlantic (ATL) basin. There are 91 (33) TCs and 113 (50) cases with CE identified in the WNP (ATL). Three CE structural change types are classified as follows: a CE with the inner eyewall dissipated in an eyewall replacement cycle (ERC, 51 and 56% in the WNP and ATL), a CE with the outer eyewall dissipated first and the no eyewall replacement cycle (NRC, 27 and 29% in the WNP and ATL), and a CE structure that is maintained for an extended period (CEM, 23 and 15% in the WNP and ATL). The moat size and outer eyewall width in the WNP (ATL) basin are approximately 20–50% (15–25%) larger in the CEM cases than that in the ERC and NRC cases. Our analysis suggests that the ERC cases are more likely dominated by the internal dynamics, whereas the NRC cases are heavily influenced by the environment condition, and both the internal and environmental conditions are important in the CEM cases. A good correlation of the annual CE TC number and the Oceanic Niño index is found (0.77) in WNP basin, with most of the CE TCs occurring in the warm episodes. In contrast, the El Niño/Southern Oscillation (ENSO) may not influence on the CE formation in the ATL basin. After the CE formation, however, the unfavorable environment that is created by ENSO may reduce the TC intensity quickly during warm episode. The variabilities of structural changes in the WNP basin are larger than that in the ATL basin.

**Keywords:** concentric eyewall, microwave satellite, ENSO

© 2016 The Author(s). Licensee InTech. This chapter is distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/3.0), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited. © 2016 The Author(s). Licensee InTech. This chapter is distributed under the terms of the Creative Commons Attribution License (http://creativecommons.org/licenses/by/3.0), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

## **1. Introduction**

Tropical cyclones (TCs), and particularly strong TCs, are observed with a concentric eyewall (CE) structure that has an inner eyewall and an outer eyewall separated by a convective minimum region [1]. A local tangential wind maximum is associated with the outer eyewall and the most rapid increase in wind speed lies on the inside of the wind maximum [1]. The outer wind maximum thus contracts and intensifies, and then the inner eyewall weakens and eventually vanishes during eyewall replacement cycle (ERC). One of the great challenges associated with TC prediction is the large variability in structure and intensity changes, and the CE formation and the ERC is a mechanism to produce such variability [1–4]. Many theories allude to the influences of both synoptic scale environmental conditions and mesoscale processes in the CE formation. Nong and Emanuel [5] showed that the CE may form due to favorable environmental condition or external forcing and wind-induced surface heat exchange instability. Examples of internal dynamics include propagating vortex Rossby waves (VRWs) that interact with a critical radius [6, 7] and axisymmetrization during a binary vortex interaction [8, 9]. Terwey and Montgomery [10] employed idealized full physics hurricane to demonstrate the secondary eyewall form at region of sufficient low-level radial potential vorticity gradient. The result highlights the VRW energy accumulation in the critical radius with a wind-moisture feedback process at the air-sea interface. Huang et al. [11] suggested that the broadening of the radial tangential wind profile above the boundary layer (BL) in a symmetric fashion can lead to BL convergence and inflow. The progressive strengthening of the BL inflow and the unbalanced BL response may lead to secondary eyewall formation. Previous observational studies indicate that the secondary eyewall can act as a barrier to the moisture inflow to the inner eyewall (e.g., [12]).

Sitkowski et al. [4] used flight-level data to study the ERC process in the Atlantic (ATL) basin. They suggested that large variances are in the ERC time requirement, the intensity, and the change in radii because CEs are not only associated with intensity but also structural changes. Maclay et al. [13] used the low-level area-integrated kinetic energy to show that while the intensity weakens during the ERC, the integrated kinetic energy and the TC size increase. Their results suggest that CE formation and ERC are dominated by internal dynamical processes. The passive microwave data can more clearly reveal the CE structure in TCs. Using microwave data between 1997 and 2002, Hawkins and Helveston [14] suggested that CEs exist with a much higher percentage (80 and 40%) in intense TCs (maximum wind > 120 kts) than previously realized in the western North Pacific (WNP) and ATL basin. As further noted by Hawkins et al. [15], there were more CE cases with large radius in the WNP than in other basins. Hawkins and Helveston [16] provided examples of different modes of CE structure, including the ERC, triple eyewalls [17], ERCs that are repeated multiple times, ERCs that are interrupted by vertical shear and landfall, and cases where an outer eyewall forms at a large radius and remains in a CE structure for a long duration. The different CE modes appear to have profound impacts on intensity and structural forecasts. This study quantitatively examines these structural and intensity changes of CE by an objective method.

There have been extensive studies on TCs in different El Niño/Southern Oscillation (ENSO) phases, and no significant correlation has been found between the annual TC genesis number and ENSO over the WNP basin (e.g., [18]). The annual genesis number, however, increases over the southeastern part of the WNP and decreases over the northwestern part in the El Niño (the warm episode) and a reversed situation occurred in the La Niña (the cold episode) [19, 20]. TCs tend to recurve toward higher latitudes in the periphery of subtropical high system before landfall due to the shift of the genesis region in the warm episode. In contrast, TCs tend to move more westward in the La Niña years ([20], and references therein). The mean duration of TCs over the ocean tends to be longer during the warm episode than that in the cold episode [21]. As a result, there are more intense and long-lived typhoons in the warm episode than in the cold episode [19, 22]. In the ATL basin, ENSO inhibits the formation of TCs through the enhancement of the vertical wind shear, subsidence, and reduced relative humidity in the tropical ATL [20, 23, 24]. Teleconnection theory suggests that warm-free tropospheric temperatures that are spread eastward from the Pacific by equatorial wave dynamics can be unfavorable to convection and can influence sea surface temperature (SST) in the ATL ([25], and references therein). As stated above, shifts in TC tracks and environmental conditions have been linked to phase changes in ENSO. Since the variations in the environment have been linked to CE characteristics [26], we examine frequency and storm structures of CE TCs in relation to ENSO.

In this chapter, we present the data, the objective CE identification method, and the CE structural and intensity changes in the WNP and ATL basins. The relationship between CE TCs and ENSO is discussed and a conclusion is presented at the end of the chapter.
