Upper tropospheric cyclonic vortex

Satellite image of an upper tropospheric cyclonic vortex in the western North Pacific

An upper tropospheric cyclonic vortex is a vortex, or a circulation with a definable center, that usually moves slowly from east-northeast to west-southwest and is prevalent across Northern Hemisphere's warm season. Its circulations generally do not extend below 6,080 metres (19,950 ft) in altitude. A weak inverted wave in the easterlies is generally found beneath it, and it may also be associated with broad areas of high-level clouds. Downward development results in an increase of cumulus clouds and the appearance of circulation at ground level. In rare cases, it becomes warm-core, resulting in the vortex becoming a tropical cyclone. Symbiotic relationships can exist between tropical cyclones and the upper level lows in their wake, with the two systems occasionally leading to their mutual strengthening. When they move over land during the warm season, an increase in monsoon rains occurs.

History of research

Using charts of mean 200-hectopascal circulation for July through August (located 9,200 metres (30,200 ft) above sea level) to locate the circumpolar troughs and ridges, it is observed that there is a trough line extending over the eastern and central North Pacific and another one extending over the North Atlantic. Walter Bohan performed case studies of upper tropospheric cyclones in the Atlantic and Pacific by using airplane reports (winds, temperatures and heights), radiosonde data, geostationary satellite cloud imagery, and cloud-tracked winds throughout the troposphere. He determined that they are an upper tropospheric cold-core low and a cut-off low.

The tropical upper tropospheric cyclone has a cold core, meaning it is stronger aloft than at the Earth's surface. It also means that a pool of cold air aloft is associated with the feature. If both an upper tropospheric cold-core low and lower tropospheric easterly wave trough are in-phase, with the easterly wave near or to the east of the upper level cyclone, thunderstorm development (also known as convection) is enhanced. If they are out-of-phase, with the tropical wave west of the upper level circulation, convection is suppressed. Upper level cyclones also interact with troughs in the subtropical westerlies, such as cold fronts and stationary fronts. When the subtropical disturbances in the Northern Hemisphere actively move southward, or dig, the area between the upper tropospheric anticyclone to its west and cold-core low to its east generally have strong northeasterly winds in addition to a rapid development of active thunderstorm activity. It is typical for cloud bands associated with the upper tropospheric cyclonic vortices to be aligned with the vertical wind shear. Animated satellite cloud imagery is a better tool for their early detection and tracking. The low-level convergence caused by the cut-off low can trigger squall lines and rough seas, and the low-level spiral cloud bands caused by the upper level circulation are alongside the low-level wind direction.

Climatology

In the Northern Hemisphere, the tropical upper tropospheric trough normally occurs between May and November, with peak activity between July and September. James Sadler suggested a revised model for the tropical upper tropospheric trough during the early part of the typhoon season in the western Pacific. He also suggested that the tropical upper tropospheric trough cyclonic cells are caused by the mid-latitude disturbance riding around the western side of the tropical upper tropospheric trough when the subtropical ridge between these systems is extraordinarily weak. In the north Atlantic, the upper tropospheric trough is characterized by the semi-permanent circulation pattern that forms in the North Atlantic between August and November. Toby Carlson evaluated data over the eastern Caribbean sea for October 1965 and pinpointed the presence of an upper tropospheric cold-core cyclone. These cold-core cyclones generally form close to the Azores and move south and westward towards a latitude of 20°N. These circulations extend over an area of about 20° of latitude (or 2,220 kilometres (1,200 nmi)) and 40° of longitude. The lowest level of closed circulation underneath the upper level cold-core cyclone is often between the 700 and the 500-hectopascal level (3,000 metres (9,800 ft) to 5,800 metres (19,000 ft) above sea level). Their life cycles span 5 to 14 days.

The upper tropospheric cyclonic centers in the North Atlantic differ from that in the North Pacific. Most of them are detectable in the low tropospheric temperature field as cold troughs in the easterlies. They tend to vertically tilt toward the northeast. Cumulonimbus clouds and rainfall occur in the southeast quadrant, approximately 5° latitude (or 555 kilometres (300 nmi)) from the upper cyclone center. Large variations of cloud cover can exist in different systems. James Sadler revealed that the summer tropical upper tropospheric trough is a dominant feature over the trade wind regions of the North Atlantic Ocean, Gulf of Mexico, and Caribbean Sea, and that the lower tropospheric responses to the tropical upper tropospheric trough in the North Atlantic are differ from those in the North Pacific.

Interaction with tropical cyclones

Pair of upper tropospheric cyclonic vortices in the Gulf of Mexico and Atlantic acting as outflow channels for Hurricane Dean in August 2007

Main article: Tropical cyclogenesis

The summer tropical upper tropospheric trough in the Southern Hemisphere lies over the trade wind region of the east central Pacific and can cause tropical cyclogenesis offshore Central America. University of Hawaii Professor James C. Sadler has documented tropical cyclones over the eastern North Pacific that were revealed by weather satellite observations, and suggested that the upper-tropospheric circulation is a factor in the development, as well as the life history, of the tropical cyclones. Ralph Huschke and Gary Atkinson proposed that a moist southwest wind that results from southeast trades of the eastern South Pacific deflecting towards the Pacific coasts of Central America between June and November, is known as the "temporale". Temporales are most frequent in July and August, when they can reach gale force and cause rough seas/swell. The area of heavy rain is generally located in the northeast quadrant approximately 5° of latitude (or 555 kilometres (300 nmi)) from the eye.

Trailing upper cyclones and upper troughs can cause additional outflow channels and aid in the intensification process of tropical cyclones. Developing tropical disturbances can help create or deepen upper troughs or upper lows in their wake due to the outflow jet stream emanating from the developing tropical disturbance/cyclone. In the western North Pacific, there are strong reciprocal relationships between the areas of formative tropical cyclones and that of the lower tropospheric monsoon troughs and the tropical upper tropospheric trough. Tropical cyclone movement can also be influenced by TUTT cells within 1,700 kilometres (920 nmi) of their position, which can lead to non-climatological tropical cyclone tracks.

Interaction with monsoon regimes

See also: Monsoon

As upper level lows retrograde over land masses, they can enhance thunderstorm activity during the afternoon. This magnifies regional monsoon regimes, such as that over western North America near the United States and Mexican border, which can be used to effectively forecast monsoon surges in precipitation magnitude. Across the north Indian ocean, the formation of this type of vortex leads to the onset of monsoon rains during the wet season.