Lake-effect snow is produced during cooler atmospheric conditions when a cold air mass moves across long expanses of warmer lake water, warming the lower layer of air which picks up water vapor from the lake, rises up through the colder air above, freezes and is deposited on the leeward (downwind) shores.
The same effect also occurs over bodies of salt water, when it is termed ocean-effect or bay-effect snow. The effect is enhanced when the moving air mass is uplifted by the orographic influence of higher elevations on the downwind shores. This uplifting can produce narrow but very intense bands of precipitation, which deposit at a rate of many inches of snow each hour, often resulting in a large amount of total snowfall.
The areas affected by lake-effect snow are called snowbelts. These include areas of the Great Lakes, the west coasts of northern Japan, the Kamchatka Peninsula in Russia, and areas near the Great Salt Lake, Black Sea, Caspian Sea, Baltic Sea, and parts of the northern Atlantic Ocean.
A lake-effect blizzard is the blizzard-like conditions resulting from lake-effect snow. Under certain conditions, strong winds can accompany lake-effect snows creating blizzard-like conditions; however the duration of the event is often slightly less than that required for a blizzard warning in both the US and Canada.
If the air temperature is low enough to keep the precipitation frozen, it falls as lake-effect snow. For lake-effect rain or snow to form, the air moving across the lake must be significantly cooler than the surface air (which is likely to be near the temperature of the water surface). Specifically, the air temperature at an altitude where the air pressure is 850 millibars (85 kPa) (roughly 1.5 kilometers or 0.93 miles vertically) should be 13 °C (23 °F) lower than the temperature of the air at the surface. Lake-effect occurring when the air at 850 millibars (85 kPa) is much colder than the water surface can produce thundersnow, snow showers accompanied by lightning and thunder (caused by larger amounts of energy available from the increased instability).
Lake-effect snow is produced as cold winds blow clouds over warm waters. There are several key elements that are required to form lake-effect precipitation and which determine its characteristics: instability, fetch, wind shear, upstream moisture, upwind lakes, synoptic (large)-scale forcing, orography/topography, and snow or ice cover.
A temperature difference of 13 °C (23 °F) (or as past researchers have estimated: between 15 °C and 25 °C) between the lake temperature and the height in the atmosphere (~1,500 meters or 4,921 feet at which barometric pressure measures 850 millibars (85 kilopascals)) provides for absolute instability and allows vigorous heat and moisture transportation vertically. Atmospheric lapse rate and convective depth are directly affected by both the mesoscale lake environment and the synoptic environment; a deeper convective depth with increasingly steep lapse rates and a suitable moisture level will allow for thicker, taller lake effect precipitation clouds and naturally a much greater precipitation rate.
The distance that an air mass travels over a body of water is called fetch. Because most lakes are irregular in shape, different angular degrees of travel will yield different distances; typically a fetch of at least 100 km (62 mi) is required to produce lake effect precipitation. Generally, the larger the fetch the more precipitation that will be produced. Larger fetches provide the boundary layer with more time to become saturated with water vapor and for heat energy to move from the water to the air. As the air mass reaches the other side of the lake, the engine of rising and cooling water vapor pans itself out in the form of condensation and falls as snow, usually within 40 kilometers (25 miles) of the lake but sometimes up to about 100 miles.
Directional shear is one of the most important factors governing the development of squalls; environments with weak directional shear typically produce more intense squalls than those with higher shear levels. If directional shear between the surface and the height in the atmosphere at which the barometric pressure measures 700 mb (70 kPa) is greater than 60 degrees, nothing more than flurries can be expected. If the directional shear between the body of water and the vertical height at which the pressure measures 700 mb (70 kPa) is between 30 and 60 degrees, weak lake-effect bands are possible. In environments where the shear is less than 30 degrees, strong, well organized bands can be expected.
Speed shear is less critical, but should be relatively uniform. The wind speed difference between the surface and vertical height at which the pressure reads 700 mb (70 kPa) should be no greater than 40 knots (74 km/h) so as to prevent the upper portions of the band from shearing off. However, assuming the surface to 700 mb (70 kPa) winds are uniform, a faster overall velocity will work to transport moisture quicker from the water, and the band will travel much farther inland.
Temperature difference and instability are directly related, the greater the difference the more unstable and convective the lake effect precipitation will be.
A lower upstream relative humidity will make it more difficult and time consuming for lake effect condensation, clouds and precipitation to form. The opposite is true if the upstream moisture has a high relative humidity, allowing lake effect condensation, cloud and precipitation to form more readily and in a greater quantity.
Any large body of water upwind will impact lake-effect precipitation to the lee of a downwind lake by adding moisture or pre-existing lake-effect bands, which can re-intensify over the downwind lake. Upwind lakes do not always lead to an increase of precipitation downwind.
Vorticity advection aloft and large upscale ascent help increase mixing and the convective depth, while cold air advection lowers the temperature and increases instability.
Orography and topography
Typically lake-effect precipitation will increase with elevation to the lee of the lake as topographic forcing squeezes out precipitation and dries out the squall much faster.
Snow and ice cover
As a lake gradually freezes over, its ability to produce lake-effect precipitation decreases for two reasons. Firstly, the open ice-free liquid surface area of the lake shrinks. This reduces fetch distances. Secondly, the water temperature nears freezing, reducing overall latent heat energy available to produce squalls. To end the production of lake-effect precipitation, a complete freeze is often not necessary.
Even when precipitation is not produced, cold air passing over warmer water may produce cloud cover. Fast moving mid-latitude cyclones, known as Alberta clippers, often cross the Great Lakes. After the passage of a cold front, winds tend to switch to the northwest, and a frequent pattern is for a long-lasting low-pressure area to form over the Canadian Maritimes, which may pull cold northwestern air across the Great Lakes for a week or more, commonly identified with the negative phase of the North Atlantic Oscillation (NAO). Since the prevailing winter winds tend to be colder than the water for much of the winter, the southeastern shores of the lakes are almost constantly overcast, leading to the use of the term The Great Gray Funk as a synonym for winter. These areas allegedly contain populations that suffer from high rates of seasonal affective disorder, a type of psychological depression thought to be caused by lack of light.
Cold winds in the winter typically prevail from the northwest in the Great Lakes region, producing the most dramatic lake-effect snowfalls on the southern and eastern shores of the Great Lakes. This lake-effect produces a significant difference between the snowfall on the southern/eastern shores and the northern and western shores of the Great Lakes.
The most affected areas include Upper Michigan, Central New York, Western New York, Northwestern Pennsylvania, Northeastern Ohio, southwestern Ontario and central Ontario, Northeastern Illinois (along the shoreline of Lake Michigan), northwestern and northcentral Indiana (mostly between Gary, IN and Elkhart, IN), and western Michigan. Tug Hill in New York’s North Country region has the 2nd most snow amounts of any non-mountainous location within the continental U.S., only trailing the Upper Peninsula of Michigan, which can average over 200 inches (508 centimeters) of snow per year.
Lake-effect snows on the Tug Hill plateau (east of Lake Ontario) can frequently set daily records for snowfall in the United States. Tug Hill receives, on average, over 20 feet (240 in; 610 cm) of snow each winter. In February 2007, a prolonged lake-effect snow event left 141 inches (358 cm) of snow on the Tug Hill Plateau. Syracuse, New York, is directly south of the Tug Hill Plateau and receives significant lake-effect snow from Lake Ontario, averaging 115.6 inches (294 cm) of snow per year, which is enough snowfall to often be considered one of the “snowiest” large cities in America.
A small amount of lake-effect snow from the Finger Lakes falls in upstate New York as well. If the wind blows almost the entire length of either Cayuga Lake or Seneca Lake, Ithaca or Watkins Glen respectfully can have a small lake effect snow storm. The Appalachian Mountains and Atlantic Ocean largely shield New York City and Philadelphia from picking up any lake-effect snow; snow there tends to come from mesocyclonic storm systems mixing with cold temperatures.
Lake Erie produces a similar effect for a zone stretching from the eastern suburbs of Cleveland through Erie to Buffalo. Remnants of lake-effect snows from Lake Erie have been observed to reach as far south as Garrett County, Maryland and as far east as Geneva, New York. Because it’s not as deep as the other lakes, Erie warms rapidly in the spring and summer and is frequently the only Great Lake to freeze over in winter. . Once frozen, the resulting ice cover alleviates lake-effect snow downwind of the lake. Based on stable isotope evidence from lake sediment coupled with historical records of increasing lake effect snow, it has been predicted that Global Warming will result in a further increase in lake effect snow.
A very large snowbelt in the United States exists on the Upper Peninsula of Michigan, near the cities of Houghton, Marquette, and Munising. These areas average 250–300 inches (635–762 cm) of snow each season. For comparison, on the western shore, Duluth, Minnesota receives 78 inches (198 cm) per season. Lake Superior and Lake Huron rarely freeze because of their size and depth; hence, lake-effect snow can fall continually in the Upper Peninsula and Canadian snowbelts during the winter months. Main areas of the Upper Peninsula snow belt include the Keweenaw Peninsula and Baraga, Marquette and Alger counties, where Lake Superior contributes to lake-effect snow, making them a prominent part of the Midwestern snow belt. Records of 390 inches (991 cm) of snow or more have been set in many communities in this area. The Keweenaw Peninsula averages more snowfall than almost anywhere in the United States—more than anywhere east of the Mississippi River and the most of all non-mountainous regions of the continental United States.
Because of the howling storms across Lake Superior, which cause dramatic amounts of precipitation, it has been said that the lake-effect snow makes the Keweenaw Peninsula the snowiest place east of the Rockies. Only one official weather station exists in this region. Located in Hancock, Michigan, this station averages well over 210 inches (533 cm) per year. Farther north in the peninsula, lake-effect snow can occur with any wind direction. The road commission in Keweenaw County, Michigan collects unofficial data in a community called Delaware, and it strictly follows the guidelines set forth by the National Weather Service. This station averages over 240 inches (610 cm) per season. Even farther north, a ski resort called Mount Bohemia receives an unofficial annual average of 273 inches (693 cm). Herman, Michigan, averages 236 inches (599 cm) of snow every year. Lake-effect snow can cause blinding whiteouts in just minutes, and some storms can last days.
Western Michigan, western Northern Lower Michigan, South shore of Lake Erie, Buffalo NY and Northern Indiana can get heavy lake-effect snows as winds pass over Lake Michigan and deposit snows over Muskegon, Traverse City, Grand Rapids, Kalamazoo, New Carlisle, South Bend, and Elkhart, but these snows abate significantly before Lansing or Fort Wayne, Indiana. When winds become northerly, or aligned between 330 and 390 degrees, a single band of lake-effect snow may form, which extends down the length of Lake Michigan. This long fetch often produces a very intense, yet localized, area of heavy snowfall, affecting cities such as Laporte and Gary.
Lake-effect snow is uncommon in Detroit, Toledo, Milwaukee, and Chicago, because the region’s dominant winds are from the northwest, making them upwind from their respective Great Lakes. However, they too can see lake-effect snow during easterly or north-easterly winds. More frequently, the north side of a low-pressure system picks up more moisture over the lake as it travels west, creating a phenomenon called lake-enhanced precipitation.
Similar snowfall can occur near large inland bays, where it is known as bay-effect snow. Bay-effect snows fall downwind of Delaware Bay, Chesapeake Bay, and Massachusetts Bay when the basic criteria are met, and on rarer occasions along Long Island.
The southern and southeastern sides of the Great Salt Lake receive significant lake-effect snow. Since the Great Salt Lake never freezes, the lake effect can influence the weather along the Wasatch Front year-round. The lake effect largely contributes to the 55–80 inches (140–203 cm) annual snowfall amounts recorded south and east of the lake, and in average snowfall reaching 500 inches (13 m) in the Wasatch Range. The snow, which is often very light and dry because of the semi-arid climate, is referred to as “The Greatest Snow on Earth” in the mountains. Lake-effect snow contributes to approximately 6–8 snowfalls per year in Salt Lake City, with approximately 10% of the city’s precipitation being contributed by the phenomenon.
The Texas twin cities of Sherman and Denison are known, in rare instances, to have experienced lake-effect snow from nearby Lake Texoma due to the lake’s size (it is the third-largest lake in Texas or along its borders).
On one occasion in December 2016, lake effect snow fell in central Mississippi from a lake band off Ross Barnett Reservoir.
The Truckee Meadows and other parts of Northern Nevada which are normally in the rain shadow of the Sierra Nevada can, when conditions are right, have severe snowfall as a result of lake effect from Lake Tahoe. Recent severe examples of this phenomenon have occurred as recently as 2004, dumping several feet of snow in the normally dry region.
The West Coast occasionally experiences ocean-effect showers, usually in the form of rain at lower elevations south of about the mouth of the Columbia River. These occur whenever an Arctic air mass from western Canada is drawn westward out over the Pacific Ocean, typically by way of the Fraser Valley, returning shoreward around a center of low pressure. Cold air flowing southwest from the Fraser Valley can also pick up moisture over the Strait of Georgia and Strait of Juan de Fuca, then rise over the northeastern slopes of the Olympic Mountains, producing heavy, localized snow between Port Angeles and Sequim, as well as areas in Kitsap County and the Puget Sound region.
Rarely, the phenomenon of gulf-effect snow has been observed along the northern coast of the Gulf of Mexico, notably during Florida’s Great Blizzard of 1899. Another extreme occurrence of “ocean effect” snow occurred on January 24, 2003, when wind off the Atlantic, combined with air temperatures in the 20 °F (−7 °C), brought snow flurries to the Atlantic coast of Florida as far south as Cape Canaveral.
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