caa a22 4500 469052872 CHVBK 20180323132835.0 cr unu---uuuuu 170328e19920301xx s 000 0 eng 10.1007/BF01025409 doi (NATIONALLICENCE)springer-10.1007/BF01025409 Tripoli G. Department of Meteorology, University of Wisconsin-Madison, 53706, Madison, Wisconsin, USA aut An explicit three-dimensional nonhydrostatic numerical simulation of a tropical cyclone [Elektronische Daten] [G. Tripoli] Summary: A nonhydrostatic numerical simulation of a tropical cyclone is performed with explicit representation of cumulus on a meso-β scale grid and for a brief period on a meso-γ scale grid. Individual cumulus plumes are represented by a combination of explicit resolution and a 1.5 level closure predicting turbulent kinetic energy (TKE). The results demonstrate a number of expected and unexpected important scale interaction processes. Within the central core of the developing cyclone, meso-β convective regions grow and breakdown into propagating inertiagravity waves throughout the lifecycle of the cyclone. In the early stages, the amplitude of pressure fluctuations associated with the meso-β scale convection exceed the central pressure of the cyclone and strongly modulate its intensity. With each meso-β scale pulsation, the cyclone core increases in strength, measured by the central pressure deficit. The increasingly strong inertial frequency of the storm core acts to increasingly trap the convection induced heating within the core by balancing the tangential wind against the low central pressure, before the meso-β scale convection breaks down and sends the warmth away as a propagating wave. Eventually, the slow manifold's amplitude exceeds the amplitude of the meso-β scale oscillations and a stable eye region is formed. As inertial instability increases, increasingly high thermal warmth can be protected in the core, allowing persistent subsidence to form and to clear out the cyclone eye. On the outside of the eye wall, strong inertial stability gradients in the troposphere cause convective warming to split the inflow to the eye wal! and spawn outwardly propagating inertia gravity waves. These waves carry away all of the heating forced by convection that is not inertially trapped by the eye wall and act as a moderating influence on storm intensity. Inertia gravity waves are also spawned in the stratosphere at the top of the eye wall by the revolution of asymmetric cumulus structures. In all instances, the tropospheric waves are coupled to the propagating stratospheric waves which both move at 35 ms−1, although there are many instances where the stratospheric waves seem to have no tropospheric counterpart. Hence the anvil top forcing and low level breakdown are linked. The outwardly propagating inertia gravity waves act to initiate outer bands of convection. This initiation is with the assistance of low level boundary layer variations of density related to previous convection and to virga falling from the anvil which moistens and destabilizes the mid levels ofθ e minimum. The convection initiated by these waves does not move substantially outward with the wave, although may appear to develop outward discontinuously. Springer-Verlag, 1992 Meteorology and Atmospheric Physics Springer-Verlag 49/1-4(1992-03-01), 229-254 0177-7971 49:1-4<229 1992 49 703 https://doi.org/10.1007/BF01025409 text/html Onlinezugriff via DOI 1 research-article jats NATIONALLICENCE 856 40 https://doi.org/10.1007/BF01025409 text/html Onlinezugriff via DOI NATIONALLICENCE 100 1- Tripoli G. Department of Meteorology, University of Wisconsin-Madison, 53706, Madison, Wisconsin, USA aut NATIONALLICENCE 773 0- Meteorology and Atmospheric Physics Springer-Verlag 49/1-4(1992-03-01), 229-254 0177-7971 49:1-4<229 1992 49 703 Metadata rights reserved Springer special CC-BY-NC licence nationallicence BK010053 XK010053 XK010000 NATIONALLICENCE NATIONALLICENCE NL-springer