1. Hurricanes in Other Climates Robert Korty Texas A&M

2. Atlantic Main Development Region SST (ASO mean) and power dissipation (whole season, whole basin) 1-3-4-3-1 filter applied to smooth interannual variability

3. Holland and Bruyere (submitted)

4. Lines of evidence: Geologic evidence (paleotempestology) Quantitative results from modeling techniques:  Global Tropical cyclones and climate Current Warmer

5. Lines of evidence: Geologic evidence (paleotempestology) Quantitative results from modeling techniques:  Global (general circulation)  Downscaling Tropical cyclones and climate

6. Lines of evidence: Geologic evidence (paleotempestology) Quantitative results from modeling techniques:  Global (general circulation)  Downscaling Thermodynamic controls from large-scale environment  Potential intensity (thermal stability of atmosphere)  Moisture (entropy) content of tropical atmosphere  Vertical wind shear Tropical cyclones and climate

7. Knutson et al. 2008 Atlantic tropical cyclone counts fall in warmer simulation Distribution is shifted towards stronger events Global models are unable to simulate intense events… Tropical cyclones and climate

8. Knutson et al. 2008 Tropical cyclone climatology in 21 st century simulations Atlantic tropical cyclone counts fall in warmer simulation Distribution is shifted towards stronger events Global models are unable to simulate intense events…

9. Bender et al. 2010 …but higher resolution models show an increase in the frequency of strong events

10. Potential Intensity of tropical cyclones Thermodynamic speed limit to a tropical cyclone’s (TC) intensity V max set by strength of fluxes from sea to atmosphere and the thermodynamic stability of the atmospheric column above Principally determined by level of neutral bouyancy, which sets T o.

11. The Last Glacial Maximum: 21,000 years ago CO 2 was 185 ppm Tropical temperatures were 2-3 o C cooler than today As much as 30 o C colder over land where there was ice

12. Storm Season potential intensity and SST Longitude Latitude

13. Storm Season potential intensity and SST Longitude Latitude

14. Similar behavior in hot climates A series of simulations in which CO 2 is progressively doubled. These start with preindustrial levels (280 ppm) and roll upward: 560, 1120, 2240, 4480, 8960. The hottest of these (8960 ppm, which is 2 5 preindustrial levels) feature tropical SST > 40 o C.

15. Changes in potential intensity and SST 2240 ppm CO 2 - control8960 ppm CO 2 - control

16. Joint distribution of SST and potential intensity

17. Joint distribution of SST and T o.

18. Joint distribution of SST and LNB.

19. What else can affect potential intensity? Anything that has an uneven response relative to a moist adiabat. This includes the response to strong volcanic eruptions and, more weakly, to the solar cycle. Following the eruption of a low-latitude volcano that explodes aerosols and particles into the stratosphere, surface climate cools over the following year while tropopause temperatures rise.

20. Simulation of the Last Millennium

21. Volcanism Seasons following 1258 eruption Kuwae (1452) Tambora (1815)

22. Seasonal cycle of PI following volcanic eruptions

23. Zonal annual mean difference in T: S max -S min Model (CCSM) Reanalysis (NCAR/NCEP)

24. Orbit varies: does this affect TC environment? Date Earth makes its closest approach to the Sun rotates around the calendar. Every 57 years it advances another day. 6000 years ago, atmospheric composition was nearly identical to its state through start of industrial revolution ca. 1870, but nearest approach to Sun occurred in September rather than January (today).

25. Lines of evidence: Geologic evidence (paleotempestology) Tropical cyclones and climate sand layer from a prehistoric hurricane Photos courtesy of Kam-biu Liu (LSU) and Jon Woodruff (U. Mass.). Hurricane Carol Great New England Hurricane Great September Gale Great Colonial Hurricane

26. TOA radiation perturbations

27. Change in Mid-Holocene potential intensity

28. Change in surface T and s at Mid-Holocene

29. Mid-Tropospheric entropy content Tropical cyclones require a supply of moist, high entropy air to maintain a saturated core. Downdrafts carry drier, low entropy air from the middle troposphere into the boundary layer. If inflow is not strong enough, these can choke off incipient events. Relevant parameter is s b -s m ~ s*-s m. Moist entropy varies with both relative humidity and temperature, and can change with climate owing to large- scale temperature variations even when RH does not.

30. Saturation Entropy Deficit