Convective inhibition (CIN or CINH) is a numerical measure in meteorology that indicates the amount of energy that will prevent an air parcel from rising from the surface to the level of free convection.
CIN is the amount of energy required to overcome the negatively buoyant energy the environment exerts on an air parcel. In most cases, when CIN exists, it covers a layer from the ground to the level of free convection (LFC). The negatively buoyant energy exerted on an air parcel is a result of the air parcel being cooler (denser) than the air which surrounds it, which causes the air parcel to accelerate downward. The layer of air dominated by CIN is warmer and more stable than the layers above or below it.
The situation in which convective inhibition is measured is when layers of warmer air are above a particular region of air. The effect of having warm air above a cooler air parcel is to prevent the cooler air parcel from rising into the atmosphere. This creates a stable region of air. Convective inhibition indicates the amount of energy that will be required to force the cooler packet of air to rise. This energy comes from fronts, heating, moistening, or mesoscale convergence boundaries such as outflow and sea breeze boundaries, or orographic lift.
CIN hinders updrafts necessary to produce convective weather, such as thunderstorms. Although, when large amounts of CIN are reduced by heating and moistening during a convective storm, the storm will be more severe than in the case when no CIN was present.
CIN is strengthened by low altitude dry air advection and surface air cooling. Surface cooling causes a small capping inversion to form aloft allowing the air to become stable. Incoming weather fronts and short waves influence the strengthening or weaking of CIN.
CIN is calculated by measurements recorded electronically by a rawinsonde (weather balloon) which carries devices which measure weather parameters, such as air temperature and pressure. A single value for CIN is calculated from one balloon ascent by use of the equation below. The z-bottom and z-top limits of integration in the equation represent the bottom and top altitudes (in meters) of a single CIN layer, Tvparcel is the virtual temperature of the specific parcel and Tvenv is the virtual temperature of the environment. In many cases, the z-bottom value is the ground and the z-top value is the LFC. CIN is an energy per unit mass and the units of measurement are joules per kilogram (J/kg). CIN is expressed as a negative energy value. CIN values greater than 200 J/kg are sufficient enough to prevent convection in the atmosphere.
The CIN energy value is an important figure on a skew-T log-P diagram and is a helpful value in evaluating the severity of a convective event. On a skew-T log-P diagram, CIN is any area between the warmer environment virtual temperature profile and the cooler parcel virtual temperature profile.
CIN is effectively negative buoyancy, expressed B-; the opposite of convective available potential energy (CAPE), which is expressed as B+ or simply B. As with CAPE, CIN is usually expressed in J/kg but may also be expressed as m2/s2, as the values are equivalent. In fact, CIN is sometimes referred to as negative buoyant energy (NBE).
- "National Weather Service Glossary - C". 21 April 2005. http://www.weather.gov/glossary/index.php?letter=c. Retrieved August 22, 2006.
- Haby, Jeff (February 28, 2004). "Ingredients for Thunderstorms and Severe Thunderstorms". The Weather Prediction.Com. http://www.theweatherprediction.com/habyhints/141/. Retrieved August 22, 2006.
- Bol, Alan (2002). "Buoyancy and CAPE". Principles of Convection I. University Corporation for Atmospheric Research. http://meted.ucar.edu/mesoprim/cape/print.htm. Retrieved August 22, 2006.
- "Skew-T Mastery". University Corporation for Atmospheric Research. http://www.meted.ucar.edu/mesoprim/skewt/cin.htm. Retrieved April 24, 2007.
- David O. Blanchard (September 1998). "Assessing the Vertical Distribution of Convective Available Potential Energy". Weather and Forecasting 13 (3): 870–877. Bibcode 1998WtFor..13..870B. doi:10.1175/1520-0434(1998)013<0870:ATVDOC>2.0.CO;2. http://ams.allenpress.com/perlserv/?request=res-loc&uri=urn%3Aap%3Apdf%3Adoi%3A10.1175%2F1520-0434%281998%29013%3C0870%3AATVDOC%3E2.0.CO%3B2.
Meteorological data and variables General Condensation Convection Temperature Pressure
Wikimedia Foundation. 2010.
Look at other dictionaries:
Convective inhibition — (dt. „Konvektionshemmung“; abgekürzt CIN, CINH) in der Meteorologie ist die Energie, die ein Luftpaket überwinden muss, um das Level of Free Convection (LFC) zu erreichen, d.h. selbständig weiter aufzusteigen. Sie ist ein Maß für die… … Deutsch Wikipedia
Convective Available Potential Energy — (CAPE) ist ein Maß für die zur Konvektion (vertikale Luftmassenbewegung) zur Verfügung stehende Energie. Sie steht in direktem Zusammenhang zur Geschwindigkeit der vertikalen Luftmassenbewegung. Höhere Werte entsprechen einem höheren Risiko für… … Deutsch Wikipedia
Convective available potential energy — A skew T plot showing a morning sounding with a large hydrolapse followed by an afternoon sounding showing the cooling which occurred in the mid levels resulting in an unstable atmosphere as surface parcels have now become negatively buoyant. The … Wikipedia
Convective instability — For a more general discussion of the same phenomenon, see Convective available potential energy. This article incorporates public domain text created by the US government. In meteorology, convective instability or stability of an airmass refers… … Wikipedia
Convective condensation level — The convective condensation level (CCL) represents the height where an air parcel becomes saturated when lifted adiabatically to achieve buoyant ascent. It marks where cloud base begins when air is heated from below to the convective temperature … Wikipedia
Convective temperature — The convective temperature (CT or Tc) is the approximate temperature that air near the surface must reach for cloud formation without mechanical lift. In such case, cloud base begins at the convective condensation level (CCL), whilst with… … Wikipedia
Free convective layer — In atmospheric sciences, the free convective layer (FCL) is the layer of conditional or potential instability in the troposphere. It is a layer of positive buoyancy (PBE) and is the layer where deep, moist convection (DMC) can occur. On an… … Wikipedia
Atmospheric convection — Conditions favorable for thunderstorm types and complexes Atmospheric convection is the result of a parcel environment instability, or temperature difference, layer in the atmosphere. Different lapse rates within dry and moist air lead to… … Wikipedia
Lapse rate — The lapse rate is defined as the rate of decrease with height for an atmospheric variable. The variable involved is temperature unless specified otherwise. The terminology arises from the word lapse in the sense of a decrease or decline;… … Wikipedia
Cloud — For other uses, see Cloud (disambiguation). Cumulus cloudscape over Swifts Creek, Australia A cloud … Wikipedia