The Proceedings of the Eighth International Conference on Creationism (2018)

stream and the associated polar front. A strong jet stream located around 35 ˚N is present over the Pacific Ocean in the reference run, Figure 7a. This is also present in the WO simulation, Figure 7b. However, when a uniform aerosol layer is added, Figures 7c and d, the jet greatly weakens because the equatorial/polar temperature contrast is reduced. There is a split in the jet, one around 25 ˚N and a stronger one at 55 ˚N. When mid-latitude aerosols (AM) are used, Figure 7e, there is no cooling of the equatorial region thus increasing the temperature contrast between the equator and the North Pole. A higher pressure gradient exists at the polar front and the strength of the jet stream is restored to strengths seen in the WO simulation. This is also true of the polar aerosols (PM), Figure 7f. Warm oceans with a uniform aerosol layer greatly reduce the jet steam; however, the rest of the warm ocean simulations (WO, AM and AP) result in stronger jet winds compared to the reference run. These jets are also shifted several degrees south in latitude. Gollmer ◀ Post-Flood Ice Age precipitation ▶ 2018 ICC 703 Figure 7. Winds associated with the jet stream during January for the following six simulations: a) Reference run b) Warm oceans c) Warm oceans stratospheric aerosols d) Warm oceans stratospheric aerosols and no ice sheets e) Warm oceans with aerosols restricted between 30˚ and 60˚ N and f) Warm oceans with aerosols restricted between 45˚ and 90˚ N. Wind vectors in these plots correspond to a 250 mb pressure level in the troposphere. Jet streams are linked to the sinking portion of the Ferrel cell (sub-tropical jet) and the rising portion of the Ferrel cell (polar jet).