Case Profile

Overview

This case begins while starting a shift at 0300 UTC on 01 Dec 2000 in the Arctic Forecasting Centre in Edmonton, Canada. Familiarize yourself with the setting for this case by reviewing the Case Profile.

Location of Interest	Hudson and Ungava Bay Region, Northern Canada
Case Time Frame	0000 UTC 01 Dec 2000-0000 UTC 03 Dec 2000
Phenomena of Interest	Polar Lows
Forecasting Challenges	Recognize the synoptic scale precursors of polar lows Recognize the low-level surface features that are conducive to the development of polar lows Recognize the development of a polar low from observations. Identify polar lows using satellite imagery Understand the limitations of model initialization and output for polar low forecasting Apply understanding of polar low steering mechanisms to a tracking forecast

Case Profile
Introduction to the case setting with a synoptic overview.

Case Challenge
A series of forecasting questions accompanied by a rich set of of data and background content to challenge forecasting skills.

Case Summary
An expert's overview of the case as it unfolded.

Resources
Bibliography and links to more information on Polar Lows.

Surface Analysis

Current Time: 0300 UTC 01 Dec 2000

It is 0300 UTC 01 Dec 2000. 0000 UTC data are available, and the new prog set has started to arrive. You are familiarizing yourself with the synoptic situation over northeastern Canada. There are only a few 0000 UTC surface observations (manned and automatic) as the smaller sites closed down for the evening at 2300 UTC.

At the surface, a low remains quasi-stationary in Baffin Bay. The low-level flow over much of northern Canada from Hudson Bay eastwards is westerly to northwesterly around this low. Surface temperatures in the source region of this flow, the Arctic Islands and across Keewatin and into northwestern Hudson Bay, are very cold, in the range of -30°C.

Click the image to view a large-format .pdf version of the CMC Surface Analysis.

500-hPa Heights and Temps

Current Time: 0300 UTC 01 Dec 2000

The 500-hPa 00-hr prog shows a low over Foxe Basin with a trough extending southwestward through western Hudson Bay. Temperatures in the trough are –39°C or colder. A well defined vorticity center is situated south of Southampton Island. These features have been moving eastward during the last 12 hours, and this motion is expected to continue. A second trough extends from the Foxe Basin low southeastwards over Baffin Island and into the Labrador Sea.

Use the check box selections to view the various fields from the GEM Regional 00-hr forecast. Or, click here to view a large-format .pdf version of the four-panel GEM Regional Charts for 0000 UTC.

Ice Analysis Chart

Current Time: 0300 UTC 01 Dec 2000

It is early December and you know that there will still be open water in many parts of the North. The current ice analysis from the Canadian Ice Service is hanging on the wall. It shows that southern and southeastern Hudson Bay still have open waters. Open water is also found in Ungava Bay, eastern Hudson Strait, and over most of the Labrador Sea.

Click the image to view the full-size ice analysis for the Hudson Bay region. For detailed information on how to interpret the ice charts, please see the Canadian Ice Service website.
(https://www.canada.ca/en/environment-climate-change/services/ice-forecasts-observations/latest-conditions.html)

NOAA-14 IR

Current Time: 0300 UTC 01 Dec 2000

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• View place names

As it is after 0000 UTC, there won’t be any POES imagery over this area until around 0800 UTC. However, you have one recent picture from 2050 UTC 30 Nov of a POES NOAA-14 IR. It shows a band of cirrus and altostratus aligned with the upper trough through Hudson Bay, and the head of a comma cloud associated with the vorticity center over Southampton Island. In some locations, surface wind directions can be inferred through the low-level streamers that have formed with the passage of cold air over open water or leads. One such example in the image is the westerly winds over western Hudson Strait.

For more information on interpreting multispectral satellite imagery, see Feature Identification Exercises: Clouds, Snow, and Ice Using MODIS. (https://www.meted.ucar.edu/npoess/modis_exercises/)

Case Challenge

Overview

From the perspective of a forecaster, respond to this series of forecast questions. The questions go through the process of identifying predevelopment, formation, and evolution of a polar low. Each question entails the use of observations, model analysis, and model prognoses. Use the Data links to pop open a new browser window displaying the data. Use the links to the Supportnig Topics for access to background information.

Use the Data links to pop open a new browser window displaying the data.
Use the links to the Supporting Topics for access to background information.

Question 1

Current Time: 0300 UTC 01 Dec 2000

Question 2

Current Time: 0300 UTC 01 Dec 2000

Question 3

Current Time: 0300 UTC 01 Dec 2000

Question 4

Current Time: 1500 UTC 01 Dec 2000

Question 5

Current Time: 0600 UTC 02 Dec 2000

Question 6

Current Time:

Question

It is now the second day of monitoring the region. The latest model run initialized at 0000 UTC 02 Dec is available. It maintains a weak area of low pressure over Ungava Bay. Examine the latest surface analysis and available observations and imagery through 0600 UTC to verify the model's six-hour forecast. Look for conditions that could lead to a polar low developing over the Ungava Bay area.

Model Data: | GEM Regional |

Observations: | AVHRR | GOES IR | Station Observations

Analysis: | Canadian Ice Service (interpretation reference) | Surface |

Forecast Approach		Projected Track
Model position of low	A	B	C
Use of steering flow at 700 hPa	A	B	C
With upper-level trough motion	A	B	C

The correct answers are shown above.

The three methods give different results. Deciding which of these is the best approach in this case is difficult. If a polar low does develop, it will be important to closely monitor its progress with satellite imagery and observations. Once the low is developed and in motion, hindsight will serve to indicate which method applies best to this case.

Model position of low - A
The model is about 50 km too far east with the polar low position in its 6-hour forecast valid 0600 UTC. Its curving track takes it to southeastern Ungava Bay by 1800 UTC. The model low fills and disappears as it moves over the peninsula.

Initialization is a key element in the model's attempts to handle polar lows. Given the sparse data in this region, the initialization may have weaknesses. As assimilation schemes improve, the model's treatment of such smaller scale systems are also improving. The judicious use of model output, with subjective corrections for initial analysis problems, is certainly a tool not to be ignored in forecasting the track of a polar low in the very short term.

Note: the model low deepening over the Labrador Sea to the east of the peninsula at this time is not the polar low; it is a separate feature.

Steering flow at 700 hPa - B
The weak steering flow indicates a slow northward motion of the polar low.

The use of a steering flow at various levels, such as 850 hPa and 700 hPa, possibly works better if the polar low is not under or very close to a sharp upper trough. In this case it is. When the low is this close to the upper trough, it is just not clear how to choose the steering flow.

Upper-level trough - C
The upper trough at 500 or 700 hPa continues to move eastward during the period. This approach moves the low eastward across Ungava Bay, the Torngat Mountains, and into the Labrador Sea.

This approach is more like a simple forecast rule used to forecast the motion of a developing synoptic scale low. A good part of the development of the polar low is related to surface and low-level effects, such as the transfer of latent and sensible heat from the open water to the atmosphere. The use of the upper trough motion will not account for these effects. In this case, it is not yet clear if it would give either a correct speed or direction of motion.

Please make a selection.

Question 7

Current Time: 1430 UTC 02 Dec 2000

Question 8

Current Time: 1430 UTC 02 Dec 2000

Case Summary

Overview

A polar low formed over the open waters of Ungava Bay early on 02 December 2000 with winds gusting up to 40 kts at some coastal observing stations. It took only a few hours for the low to form and it lasted around 20 hours. As the low slowly drifted eastward, it decayed into an area of convection over the Torngat Mountains and the Labrador Sea.

The polar low formed as a consequence of the superimposition of upper-level conditions with favourable surface conditions. Very cold air at upper and low levels, together with an area of positive vorticity advection, interacted with a low-level baroclinic zone. The baroclinic zone set up as a result of the ice/water boundary near the western shore of Ungava Bay. The open water provided large amounts of latent and sensible heating to the boundary layer, resulting in an unstable thermal profile through a deep layer of the atmosphere. The resulting polar low moved across the Bay and eventually dissipated as surface and upper-level conditions became less favourable.

Note: This Summary provides an overview of the formation, evolution, and decay of the polar low. The Case ChallengeCase Challenge provides a more in-depth analysis. Additional information on polar lows is referenced in the Supporting Topics.

Upper-level Precursors

One precursor in many polar low events is an upper-level trough containing very cold air. A rule of thumb is that the temperature in the trough at 500 hPa must be close to or below -40°C (see 1.3.1 Pre-development Conditions and 5.1.2 Identifying Pre-development Conditions). A triggering mechanism that provides some upward vertical motion, such as an area of PVA, is required to set things in motion (see 5.1.6 Identifying Trigger Mechanisms).

At 0000 UTC on 01 December the analysis indicates a 500-hPa trough lying over Foxe Basin and northern Hudson Bay. A well-defined vorticity center lies just south of Southampton Island, with an associated region of PVA to its east and south. Temperatures in the trough are very cold, near -40°C.

Upper-level Precursors (cont.)

The area of vorticity advection is well-correlated to a band of clouds composed of cirrus or thin mid-level clouds, as shown on the NOAA-14 IR imagery from 2050 UTC on 30 November.

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Lower-level Precursors

Polar lows often form due to the interaction of a suitable upper-level pattern with favourable low-level and surface conditions. Typically, these low-level conditions consist of outbreaks of cold air across ice-water boundaries and their associated low-level baroclinic zones (see 1.1.1 Sensible and Latent Heat and 1.1.2 Baroclinic Instability).

At 0000 UTC on 01 December, the surface chart shows a trough of low pressure over Foxe Basin and northern Hudson Bay. Observed temperatures are at or below -25°C west of the trough. To the east, over the Quebec coast of Hudson Bay, temperatures are higher. These conditions point to a cold-air outbreak behind the trough.

Lower-level Precursors (cont.)

The ice analysis chart for this time period shows Ungava Bay to be nearly ice free, though there is a narrow band of 9/10ths ice cover along its western and southern shores. The ice-water boundary creates a local, shallow baroclinic zone. This is enhanced at 925 hPa and 850 hPa by similarly-oriented baroclinic zones created by the cold low-level air flowing eastward over the Bay.

Triggers and Development: Upper-level Circulation

Provided that a trigger mechanism is available, polar lows typically form under a cyclonic upper-level circulation (see 1.1.4 The Cold Upper Trough and/or Cold Low).

In this case, the upper-level and surface troughs are moving eastward together and arrive near the western shore of Ungava Bay shortly before 0000 UTC on 02 December. At that time, the upper pattern is still favourable as a polar low precursor and the area of positive vorticity advection remains well-defined.

Triggers and Development: Verification

This satellite imagery shows the cloud pattern associated with the upper trough and vorticity advection as it moves eastward over Ungava Bay. Surface observations indicate the passage of the low-level trough between 1800 and 0000 UTC on 01-02 December with the associated westerly winds and cold advection to the west of the trough. From the NOAA-12 IR 2211 UTC satellite imagery, it is clear that cloud streamers are forming over the open water of western Ungava Bay in the cold westerly flow following the passage of the trough.

Triggers and Development: Upper- and Lower-level Interaction

The interaction of certain upper- and lower-level patterns is thought to be important for polar low development and can be examined in a number of ways. One method is the potential vorticity (PV) approach. PV can be used to schematically illustrate how upper-level baroclinicity can reach down in the atmosphere to link up with low-level baroclinicity. In the case of a polar low, the diabatic heating of the cold atmosphere by open water plays a key role.

Over southwestern Ungava Bay, the GEM regional 6-hour forecast from 0000 UTC on 02 December defines fluxes of up to 600 watts/m² leading to diabatic heating in the lower layers of the atmosphere.

Triggers and Development: Upper- and Lower-level Interaction (cont.)

This cross section over Ungava Bay shows PV for the same 6-hour forecast. The 1.2 PVU contour extends downward to around 800 hPa, while another small 1.2 PVU contour is found from about 1000 to 900 hPa over Ungava Bay. This low-level PV max is likely related to the diabatic heating in that area. The 1.2 PVU contour symbolically connects the upper and lower PV maxima. The interaction between upper and lower PV maxima is one way to consider the relationship between upper and lower levels in the polar low development process.

Appearance in Satellite Imagery

Polar lows form in high-latitude areas over oceans or other bodies of water. These are generally data sparse areas, making satellite imagery the primary method of detecting polar lows. Images from polar orbiters are commonly used, while those from geostationary satellites can be used if the low is not too far north. (see 3.1.4 Satellite Imagery Characteristics and 3.2 Use of Satellite Imagery)

By 0515 UTC, the GOES IR imagery shows the old comma cloud rapidly spinning up and beginning to form a more distinct spiral-shape over Ungava Bay. At the height of its development, around 0900 UTC, the polar low has a classic shape with spiral arms whose individual elements have well-defined edges typical of convective cloud.

Surface and Upper-air Observations

Due to their remote location, the forecaster will be lucky to get a ship, buoy, or coastal land station observation close to a polar low. This calls for careful monitoring of all available surface observations for subtle signs involving pressure or wind speed and direction. (See 3.1 Nowcasting)

The GEM Regional surface analysis for 1200 UTC on 02 December does not resolve the polar low. Its MSL pressure is about 1008 hPa at WKW, and 1007 at WRH. The automated analysis shows only an open trough between those two stations, with pressures no lower than 1005 hPa in the trough. In reality, pressure at WKW is 1005 hPa, 3 hPa deeper than the initialization. The observed pressure at WRH is 1008 hPa. The gradient between the stations is tighter than shown by the initialization. In addition, observed winds at WRH are westerly, indicating a closed low rather than the open trough of the initialization.

Click the following link to view a more complete set of station observations:
Station Map and Observations

Surface and Upper-air Observations (cont.)

It is very unusual to have a radiosonde observation in the vicinity of a polar low. However, in this case, the station YVP, on the south shore of Ungava Bay, did provide soundings representative of the conditions over Ungava Bay during the development of the polar low. The sounding from this site at 1200 UTC on 02 December illustrates the vertical structure of the very cold air mass in the area. The temperatures between 600 and 500 hPa are near -40ºC, and the lowest level air is at around -18ºC. This air mass, when placed over the open water of Ungava Bay, will exhibit a great deal of instability through a deep atmospheric layer.

Click the following link to view a more complete set of station observations:
Station Map and Observations

Model Initialization

It is important to realize the limitations of the NWP guidance. In December 2000, the horizontal resolution of the GEM regional model was 24 km. Since at least 8 grid points are required to define a feature in an NWP model if it is to be well-forecast, wavelike structures with a scale of around 200 km, the approximate size of Ungava Bay, are at the limit of the model's ability. (See A 20 km Grid Accurately Depicts 40 km Features in the Ten Common NWP Misconceptions series for more discussion of this point).

NWP models depend on accurate initial analyses, but the high-latitude areas in which polar lows form are generally data-sparse areas in terms of traditional observational data. This means that model trial fields (first-guess fields) can be inadequate in these areas. Satellite data have barely started to fill the data void. For these reasons, the initial analysis of a NWP model can be incorrect on the details of position and depth of a small-scale high-latitude feature such as a polar low.

Another potential analysis problem is with the ice coverage used by the model. Ice analyses may be done on relatively coarse grids, so features such as ice-water boundaries can be "smeared out," even if there are adequate ice observations. During the polar low event, there is a discrepancy between the amount of ice coverage used by the GEM Regional model versus the coverage as interpreted by the Canadian Ice Service. Since the latter is based more closely on actual observations, it is considered a more accurate representation. Compare the GEM Regional analysis for the following 00-hour forecasts to the Canadian Ice Service product.

Dissipation

Polar lows will quickly lose their strength and decay as they cross over land or ice surfaces. (See1.3.5 Dissipation of Polar Lows and 5.1.9 Forecasting the Dissipation of Polar Lows)

As noted earlier, the Ungava Bay polar low dissipated as it crossed over the Torngat Mountains. By 1800 UTC, as the polar low moves eastward with the 500 hPa trough, it loses its shape and definition as it makes landfall on the east side of Ungava Bay. It then dissipates over the land of the Torngat mountains. The upper support also moved across the Torngats to the Labrador Sea, where a rather disorganized cyclonic surface pattern formed. The polar low did not reestablish itself over the Labrador Sea. Rather, the cyclonic pattern is best considered as a new and weaker system to the lee of the Torngats.

Resources

A special thanks to Ron Goodson and Ed Hudson with the MSC for all of their efforts in data collection, content writing, and review.

The following resources were used in compiling the Support Topics for this project:

Agee, Ernest M. and Steven R. Gilbert, 1989: An aircraft investigation of mesoscale convection over Lake Michigan during the 10 January 1984 cold air outbreak. J. Atmos. Sci., 46 , No.13, 1877–1897.

Anderson, R.K., J.P. Ashman, F. Bittner, G.R. Farr, E.W. Ferguson, V.J. Oliver, and A.H. Smith, 1969: Applications of meteorological satellite data in analysis and forecasting. ESSA Tech. Rep. NESC 51 [NTIS AD-697 033].

Bader, M.J., G.S. Forbes, J.R. Grant, R.B.E. Lilley, and A.J. Waters, 1995: Images in Weather Forecasting. Cambridge University Press.

Broadfoot, D. 1990: 12 December 1989. Lake Superior polar low, unpublished presentation.

Businger, Steven, 1987: The synoptic climatology of polar low outbreaks over the Gulf of Alaska and the Bering Sea. Tellus, 39A , 307-325.

Businger, S. and R. Reed, 1989: Cyclogenesis in cold air masses. Wea. Forecasting, 4. No. 2, 133-156.

Carleton, Andrew, 1985: Satellite climatological aspect of the "polar low" and "instant occlusion."Tellus, 37A , 433-450.

Charney, J. and A. Eliassen, 1964: On the growth of the hurricane depression. J. Atmos. Sci., 21, 68-75.

COMET Module: Satellite Meteorology: GOES Channel Selection. [Available online at hhttps://www.meted.ucar.edu/satmet/goeschan/]

Duncan, C.N., 1978: Baroclinic instability in a reversed shear flow. Meteor. Mag. 107, 17-23.

Emanuel, Kerry, A., 1986: A two stage air sea interaction theory for polar lows. Proc., The Third International Conference on Polar Lows, Norway.

Emanuel, Kerry A. and Richard Rotunno, 1989: Polar lows as arctic hurricanes. Tellus, 41A , 1-17.

Hanley, D. and W.G. Richards, 1991: Polar Lows in Atlantic Canadian Waters 1977 - 1989. Report: MAES 2-91. Scientific Services Division, Atlantic Region, Atmospheric Environment Service.

Harrold, T.W. and K.A. Browning, 1969: The polar low as a baroclinic disturbance. Quart. J. Roy. Meteor. Soc., 95, 710-723.

Heinemann, Günther, 2001: Newsletter of the European Polar Low Working Group, September 2001.

Heinemann, Günther, 2003: Proc. European Geophysical Society (EGS) Polar Low Workshop, Cambridge, UK, 11-13 June 2003.

Heinemann, G., 2003. Interaction of katabatic winds, mesocyclones and sea ice formation. Proc. Ninth meeting of the EGS Polar Lows Working Group, Cambridge, UK.

Hewson, T.D., G.C. Craig, and C. Claud, 2000: Evolution and mesoscale structure of a polar low outbreak, Quart. J.Roy. Meteor. Soc., 126, 1031-1063.

Holton, James, R., 1992: Introduction to Dynamic Meteorology. 3d ed. Academic Press Ltd., London, U.K.

Lystad, M., 1986: Polar lows in the Norwegian, Greenland and Barents Sea - Final Report. Norwegian Meteorological Institute, Oslo, Norway, 196 pp.

Mailhot J., D. Hanley, B. Bilodeau, and O. Hertzman, 1996: A numerical case study of a polar low in the Labrador Sea. Tellus, 48A , 383-402.

Midtbø, K.H., 1986: Polar low forecasting. Proc. Third International Conference on Polar Lows , Norway.

Moore, G.W.K., M.C. Reader, J. York, and S. Sathiyamoorthy, 1996: Polar lows in the Labrador Sea: A case study. Tellus, 48A, 17-40.

Moore, Richard W. and T.H. Vonder Haar, 2003: Diagnosis of a polar low warm core utilizing the Advanced Microwave Sounding Unit. Wea. Forecasting, 18, 700-711.

Mullen, S., 1983: Explosive cyclogenesis associated with cyclones in polar air streams. Mon. Wea. Rev., 111, 1537-1553.

Naval Tactical Applications Guide. Vol. 8. Part 2, Arctic. East Siberian/Chukchi/Beaufort Seas. NRL/PU/7541 92-0005.

Noer, G. and M. Ovhed, 2003: Forecasting of polar lows in the Norwegian and the Barents Sea. Proc. Ninth meeting of the EGS Polar Lows Working Group, Cambridge, UK.

Nordeng, Thor Erik, and Erik A. Rasmussen, 1992: A most beautiful polar low: A case study of a polar low development in the Bear Island region. Tellus, 44A, 81-99.

Øakland, Hans, 1989: On the genesis of polar lows. Polar and Arctic Lows. Twitchell, P., E. Rasmussen, and K. Davidson, Eds., A. Deepak Publishing.

Online Manual of Synoptic Satellite Meteorology, Central Institute for Meteorology and Geodynamics, Zentralanstalt für Meteorologie und Geodynamik. [Available online at http://www.zamg.ac.at/docu/satmanu4.0/satmanu/manual/PL/pl0.htm]

Parker, Neil, 1997: Cold Air Vortices and Polar Low Handbook for Canadian Meteorologists . Environment Canada.

Parker, M.N. and Edward Hudson, 1991: Polar Low Handbook for Canadian Meteorologists. Environment Canada, Atmospheric Environment Service.

Parker, M.N, 1992: Polar lows in the Beaufort Sea and Davis Strait. Proc. Applications of New Forms of Satellite Data in Polar Low Research, Polar Low Workshop, Hvanneyri, Iceland.

Rasmussen, Erik A. and P.D. Aakjær, 1989: Two polar lows affecting Denmark. Vejret, Special Issue in English, The Danish Meteorological Society.

Rasmussen, Erik A., John Turner, and Paul Twitchell, 1992: Applications of new forms of satellite data in polar low research. Bull. Amer. Meteor. Soc., 74, 1057-1073.

Rasmussen, Erik A., and Anette Cederskov, 1994: Polar lows: A critical analysis. The life cycles of extratropical cyclones. Vol. 111. Proc. of an International Symposium, Bergen, Norway.

Rasmussen, Erik A., 1995: Polar Lows News - The Newsletter of the EGS Polar Lows Working Group. June 9, 1995, No 5. Dr. G. Heinemann, Chairman.

Rasmussen, Erik A., Chantal Claud, and James F. Purdom, 1996: Labrador Sea polar lows. The Global Atmosphere and Ocean System, Vol. 4, 275-333.

Rasmussen, Erik A., and John Turner, 2003: Polar Lows: Mesoscale Weather Systems in the Polar Regions, Cambridge University Press.

Reed, R., 1979: Cyclogenesis in polar air streams. Mon. Wea. Rev., 107, 38-52.

Reed, R. and C. Duncan, 1987: Baroclinic instability as a mechanism for serial development of polar lows: A case study. Tellus, 39A, 376-384.

Renfrew, Ian, G.W.K. Moore, and Aashish A. Clerk, 1996: Binary interactions between polar lows. Submission to Tellus, 22 November 1996; also Extended Abstract, Workshop on Theoretical and Observational Studies of Polar Lows, St. Petersburg, Russian Federation, 23-26 September 1996.

Shapiro, M.A., L.S. Fedor, and Tamara Hampel, 1987: Research aircraft measurements of a polar low over the Norwegian Sea. Tellus, 39A, 272-306.

Shapiro, M.A., T. Hampel, and L.S. Fedor, 1989: Research aircraft observations of an arctic front over the Barents Seas. Polar and Arctic Lows, Polar and Arctic Lows. Twitchell, P., E. Rasmussen, and K. Davidson, Eds., A. Deepak Publishing.

Wilhelmsen, K., 1985: Climatological study of gale-producing polar lows near Norway. Tellus, 37A, 451-459.

Yarnal, B. and Henderson, G., 1988: A satellite-derived climatology of polar-low evolution in the North Pacific. Int. J. Climatology, 9, 551-566.

Zick, 1983: Method and results of an analysis of comma cloud developments by means of vorticity fields from upper tropospheric satellite wind data. Meteor. Rundsch. 36, 69-84.

Contributors

COMET Sponsors

• Air Force Weather Agency (AFWA)
• Environment Canada Meteorological Service of Canada (MSC)
• National Environmental Satellite, Data, and Information Service (NESDIS)
• Naval Meteorology and Oceanography Command (NMOC)
• National Oceanic and Atmospheric Administration (NOAA)
• National Weather Service (NWS)

Principal Science Advisors

• Patrick Dills — UCAR/COMET
• Ron Goodson — MSC
• Noer Gunnar — Norwegian Meteorological Institute
• Ed Hudson — MSC
• Garry Toth — MSC
• Julie Turner — UK MetOffice

Project Lead/Instructional Design

• Bruce Muller — UCAR/COMET
• Patrick Parrish — UCAR/COMET

Multimedia Authoring

• Bruce Muller — UCAR/COMET
• Dan Riter — UCAR/COMET

Audio Editing/Production

• Seth Lamos — UCAR/COMET

Audio Narration

• Dan Riter — UCAR/COMET

Computer Graphics/Interface Design

• Heidi Godsil — UCAR/COMET

Illustration/Animation

• Steve Deyo — UCAR/COMET

Software Testing/Quality Assurance

• Michael Smith — UCAR/COMET

Copyrights Administration

• Lorrie Fyffe — UCAR/COMET

Data

• MSC
• NWS - NOAA

COMET HTML Integration Team 2021

• Tim Alberta — Project Manager
• Dolores Kiessling — Project Lead
• Steve Deyo — Graphic Artist
• Ariana Kiessling — Web Developer
• Gary Pacheco — Lead Web Developer
• David Russi — Translations
• Tyler Winstead — Web Developer

COMET Staff, 2004

Director

• Dr. Timothy Spangler

Deputy Director

• Dr. Joe Lamos

Business Manager/Supervisor of Administration

• Elizabeth Lessard

Administration

• Lorrie Alberta
• Heather Hollingsworth
• Bonnie Slagel

Graphics/Media Production

• Steve Deyo
• Heidi Godsil
• Seth Lamos
• Dan Riter

Hardware/Software Support and Programming

• Tim Alberta (Supervisor)
• James Hamm
• Karl Hanzel
• Andrew Jurey (Student)
• Ken Kim
• Mark Mulholland
• Carl Whitehurst

Instructional Design

• Patrick Parrish (Supervisor)
• Dr. Alan Bol
• Lon Goldstein
• Dr. Vickie Johnson
• Bruce Muller
• atherine Olson
• Dwight Owens
• Dr. Sherwood Wang

Meteorologists

• Dr. William Bua
• Patrick Dills
• Tom Dulong
• Kevin Fuell
• Patrick Hofmann (Student)
• Dr. Stephen Jascourt
• Matthew Kelsch
• Dolores Kiessling
• Heather McIntyre (Student)
• Wendy Schreiber-Abshire
• Dr. Doug Wesley

Software Testing/Quality Assurance

• Michael Smith (Coordinator)

National Weather Service COMET Branch

• Anthony Mostek (NWS COMET Branch Chief [acting] and Satellite Training Leader)
• Brian Motta
• Dr. Robert Rozumalski (SOO Science and Training Resource [SOO/STRC] Coordinator)
• Shannon White (IFPS Training)

Meteorological Service of Canada Visiting Meteorologists

• Peter Lewis
• Garry Toth