Willoughby, Marks, and Feinberg (1984) describe the regions of convection that develop in both the core of a hurricane (within 100 km of the circulation center), and in the outer rainbands that can extend more than 360 km from the circulation center of the storm. Convection is enhanced by increased surface friction along the coastline during landfall (Tuleya, 1994; Frank & Ritchie, 1999), and fast tangential winds can advect moisture counterclockwise into the left front quadrant in the core of a hurricane (Parrish, Burpee, Marks, & Grebe, 1982). Konrad, Meaux, and Meaux (2002) found that intense TCs have increased rainfall near the core of the storm. On the other hand, tropical depressions have very little organized convection in their core (Frank & Ritchie, 1999). These findings suggest that storm intensity could exhibit a strong relationship with both the location of convection relative to the circulation center of the storm and the size of the area covered by convective rainfall.