Deep Freeze 6.61 Free Download

[Camie Fons]

Asthe On Board Monitor is broken you can plug in an external Monitor tot he NB and use that to see what you are doing. You however may be required to use a Key Combination to switch screens depending on your Make & Model Note Book. ?

in order to delete deepfreeze:

1- press (ctrl-alt-delete) all at once

or right click on the taskbabr and select

task manager.

2- after the task manager windows opens up click on processes.

3- look for Frzstate2k.exe then right click on it then click on end process tree

4- also look for DFserv.exe right click then click on end process tree

5- now go to my computer and click on it, select the c: driver then click on program files

6- look for this file Faronics and delete it

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As October drew to a close, freezing progressed rapidly in the Laptev Sea. In the Antarctic, where spring is slowly unfolding, overall ice extent is low, with patterns suggesting a strong persistent low atmospheric pressure in the Amundsen Sea.

Ice extent increased at a below average rate at the beginning of the month, and open water persisted for some time in the Laptev Sea, whereas the East Siberian Sea was among the first regions to freeze up. In the last ten days of the month, ice extent rapidly increased (Figure 1b) as the Laptev Sea iced over. The delayed freeze up in the Laptev Sea could be partly a result of ocean heating from the extended period of open water this past spring and summer. However, slow freeze up in this region in recent years is also consistent with observations of eddies within the Arctic Circumpolar Boundary Current that maintain a generally upward ocean heat flux, bringing warm Atlantic water along the eastern Arctic continental slope. The Arctic Circumpolar Boundary Current is a shallow, 200- to 400-meter-deep (660 to 1,300 feet) eastward-flowing current that follows the edge of the continental shelf and carries warm water at 2 to 3 degrees Celsius (36 to 37 degrees Fahrenheit) in shallow depths around the Arctic Ocean. The configuration of the continental shelf in the Russian Arctic brings this water very near the coastal Laptev Sea.

Air temperatures during October at the 925 millibar level (approximately 2,500 feet above the surface) were near to above average over most of the Arctic Ocean (Figure 2a). The largest departures from average for this time of year were over the Kara Sea, where air temperatures averaged for October remained above freezing.

The average atmospheric circulation pattern was dominated by below average sea level pressure over nearly the entire Arctic (Figure 2b). Pressures were as much as 10 to 12 millibars below average over the Chukchi and East Siberian Seas and stretching across the pole. This pattern is reflected in the persistence of positive values of the Arctic Oscillation Index for most of the month. When the Arctic Oscillation is in its positive mode, pressures are below average over the Arctic, but above average over the Northern Hemisphere mid latitudes.

The downward linear trend in October sea ice extent over the 45-year satellite record is 80,400 square kilometers (31,000 square miles) per year, or 9.6 percent per decade relative to the 1981 to 2010 average. Based on the linear trend, since 1979 October has lost 3.46 million square kilometers (1.34 million square miles). This equivalent to about twice the size of the state of Alaska.

El Nio is an important departure in ocean temperatures along the equator, linked to weakened trade winds. During an El Nio, the cold upwelled waters along the coast of the Americas and much of the eastern parts of the tropical Pacific are replaced by warmer water. This can have global impacts on weather, ecosystems, and economies around the world by shifting the Pacific jet stream southwards. In North America, this usually results in drier and warmer conditions than usual in the northern areas, and wetter conditions in the south. While episodes of El Nio typically occur every two to seven years and can last several months to more than a year, climate model simulations by colleagues at the University of Albany suggest that the frequency of El Nio events could increase by 35 percent by the end of this century if the Arctic Ocean loses its summer ice cover.

This link was found to result from increased heat transfer from the ocean to the atmosphere in the absence of sea ice, intensifying low-pressure systems in the Bering Sea (in the area of the Aleutian Low). Lower sea level pressure increases wind speeds that may oppose trade winds, bringing warm western Pacific water towards the east. Another possible mechanism is that as the Arctic Ocean warms from losing its sea ice cover, ocean currents weaken from the south that bring warm water from the eastern Pacific toward the Arctic. Analysis with other climate models is necessary to test the robustness of these connections.

Extent is far below average in the Bellingshausen Sea, and far above average in the Amundsen and eastern Ross Seas, a pattern indicative of a strong Amundsen Sea Low. Sea level pressures in the region have been 8 to 12 millibars below average. However, sea ice extent is also low along the Wilkes Land coast, where air temperatures have been 1 to 4 degrees Celsius (2 to 7 degrees Fahrenheit) above average.

Arctic Sea Ice News & Analysis (ASINA) is produced by the National Snow and Ice Data Center (NSIDC), which is part of the Cooperative Institute for Research in Environmental Sciences (CIRES) at the University of Colorado Boulder. Researchers Walt Meier, Ted Scambos, Mark Serreze, and Julienne Stroeve regularly contribute to ASINA, sometimes featuring guest authors, and with support from Kevin Beam, Andy Barrett, Lisa Booker, Michael Brandt, Florence Fetterer, Matt Fisher, Agnieszka Gautier, Marin Klinger, Jonathan Kovarik, Jed Lenetsky, Luis Espinosa Lopez, Audrey Payne, Bruce Raup, Matt Savoie, Trey Stafford, Bruce Wallin, and Ann Windnagel.

The NASA award NNX16AJ92G funds the ASINA project. The sea ice data for the Sea Ice Index are from the NASA Snow and Ice Distributed Active Archive Center (DAAC), which is funded by NASA award 80GSFC18C0102, and from the CIRES cooperative agreement with NOAA, which is funded by NOAA NA15OAR4320137.

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