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Encyclopedia > Planetary boundary layer

The planetary boundary layer (PBL), also known as the atmospheric boundary layer (ABL) or peplosphere, is the lowest part of the atmosphere and its behavior is directly influenced by its contact with a planetary surface. It responds to surface forcings in a timescale of an hour or less. In this layer physical quantities such as flow velocity, temperature, moisture etc., display rapid fluctuations (turbulence) and vertical mixing is strong. Above the PBL is the "free atmosphere" where the wind is approximately geostrophic (parallel to the isobars) while within the PBL the wind is affected by surface drag and turns across the isobars. The free atmosphere is usually non turbulent, or only intermittently turbulent. View of Jupiters active atmosphere, including the Great Red Spot. ... In fluid dynamics, turbulence or turbulent flow is a flow regime characterized by chaotic, stochastic property changes. ... Geostrophic current a current resulting from the balance between gravitational forces and the Coriolis effect. ... In physics, the drag equation gives the drag experienced by an object moving through a fluid. ...

Contents

Cause of surface wind gradient

See also: Wind shear, wind gradient, and Ekman layer

Typically, due to aerodynamic drag, there is a wind gradient in the wind flow just a few hundred meters above the the earth's surface—the surface layer of the planetary boundary layer. Wind speed increases with increasing height above the ground, starting from zero[1] due to the no-slip condition.[2] Flow near the surface encounters obstacles that reduce the wind speed, and introduce random vertical and horizontal velocity components at right angles to the main direction of flow.[3] This turbulence causes vertical mixing between the air moving horizontally at one level and the air at those levels immediately above and below it, which is important in dispersion of pollutants[4] and in soil erosion.[5] Cirrus uncinus ice crystal plumes showing high level wind shear, with changes in wind speed and direction. ... A wind gradient describes the change in velocity and/or direction of the wind in a certain direction. ... It has been suggested that this article or section be merged with Ekman spiral. ... Aerodynamics is a branch of fluid dynamics concerned with the study of gas flows, first analysed by George Cayley in the 1800s. ... In physics, the drag equation gives the drag experienced by an object moving through a fluid. ... The surface layer is the top layer in a body of water, such as an ocean. ... In fluid dynamics, the no-slip condition states that fluids stick to surfaces past which they flow. ... In fluid dynamics, turbulence or turbulent flow is a flow regime characterized by chaotic, stochastic property changes. ... In physics, a dynamical system is said to be mixing if the phase space of the system becomes strongly intertwined, according to at least one of several mathematical definitions. ... Pollutants are substances which directly or indirectly damage us or the environment. ... Severe soil erosion in a wheat field near Washington State University, USA. Erosion is the displacement of solids (soil, mud, rock, and so forth) by the agents of wind, water, ice, or movement in response to gravity. ...


The reduction in velocity near the surface is a function of surface roughness, so wind velocity profiles are quite different for different terrain types.[2] Rough, irregular ground, and man-made obstructions on the ground, retard movement of the air near the surface, reducing wind velocity.[6][7] Because of low surface roughness on the relatively smooth water surface, wind speeds do not increase as much with height above sea level as they do on land.[8] Over a city or rough terrain, the wind gradient effect could cause a reduction of 40% to 50% of the geostrophic wind speed aloft; while over open water or ice, the reduction may be only 20% to 30%.[9] [10] The geostrophic wind is defined as the wind resulting from the balance between the Coriolis force and the pressure gradient force. ...


For engineering purposes, the wind gradient is modeled as a simple shear exhibiting a vertical velocity profile varying according to a power law with a constant exponential coefficient based on surface type. The height above ground where surface friction has a negligible effect on wind speed is called the "gradient height" and the wind speed above this height is assumed to be a constant called the "gradient wind speed".[7][11][12] For example, typical values for the predicted gradient height are 457 m for large cities, 366 m for suburbs, 274 m for open terrain, and 213 m for open sea.[13] Engineering is the applied science of acquiring and applying knowledge to design, analysis, and/or construction of works for practical purposes. ... Simple shear Simple shear is a special case of deformation of a fluid where only one component of velocity vectors has a non-zero value: And the gradient of velocity is perpendicular to it: , where is the shear rate and: The deformation gradient tensor for this deformation has only one... See Also: Watt In physics, a power law relationship between two scalar quantities x and y is any such that the relationship can be written as where a (the constant of proportionality) and k (the exponent of the power law) are constants. ... In mathematics, exponentiation is a process generalized from repeated multiplication, in much the same way that multiplication is a process generalized from repeated addition. ...


Although the power law exponent approximation is convenient, it has no theoretical basis.[14] When the temperature profile is adiabatic, the wind speed should vary logarithmically with height,[15] Measurements over open terrain in 1961 showed good agreement with the logarithmic fit up to 100 m or so (within the surface layer), with near constant average wind speed up through 1000 m.[16] Logarithms to various bases: is to base e, is to base 10, and is to base 1. ... The Log wind profile is a mathematical relationship used to approximate the general logarithmic profile of wind speeds as they increase with increasing distance from the ground. ... The surface layer is the top layer in a body of water, such as an ocean. ...


The shearing of the wind is usually three-dimensional,[17] that is, there is also a change in direction between the 'free' pressure-driven geostrophic wind and the wind close to the ground.[18] This is related to the Ekman spiral effect. The cross-isobar angle of the diverted ageostrophic flow near the surface ranges from 10° over open water, to 30° over rough hilly terrain, and can increase to 40°-50° over land at night when the wind speed is very low.[10] Shearing in continuum mechanics refers to the occurrence of a shear strain, which is a deformation of a material substance in which parallel internal surfaces slide past one another. ...  Ekman spiral effect. ...


After sundown the wind gradient near the surface increases, with the increasing stability.[19] Atmospheric stability occurring at night with radiative cooling tends to contain turbulent eddies vertically, increasing the wind gradient.[5] The magnitude of the wind gradient is largely influenced by the height of the convective boundary layer and this effect is even larger over the sea, where there is no diurnal variation of the height of the boundary layer as there is over land.[20] In the convective boundary layer, strong mixing diminishes vertical wind gradient.[21] Radiative cooling is the condition in which a body loses more energy by radiation than it gains from its surroundings. ...


Layers within PBL

As Navier-Stokes equations suggest, the planetary boundary layer turbulence is produced in the layer with the largest velocity gradients that is at the very surface proximity. This layer - conventionally called a surface layer - constitutes about 10% of the total PBL depth. Above the surface layer the PBL turbulence gradually dissipates, losing its kinetic energy to friction as well as converting the kinetic to potential energy in a density stratified flow. The balance between the rate of the turbulent kinetic energy production and its dissipation determines the planetary boundary layer depth. The PBL depth varies broadly. At a given wind speed, e.g. 8 m/s, and so at a given rate of the turbulence production, a PBL in wintertime Arctic could be as shallow as 50 m, a nocturnal PBL in mid-latitudes could be typically 300 m in thickness, and a tropical PBL in the trade-wind zone could grow to its full theoretical depth of 2000 m. The Navier-Stokes equations, named after Claude-Louis Navier and George Gabriel Stokes, are a set of equations which describe the motion of fluid substances such as liquids and gases. ... The surface layer is the top layer in a body of water, such as an ocean. ...


In addition to the surface layer, the planetary boundary layer also comprises the PBL core (between 0.1 and 0.7 of the PBL depth) and the PBL top or entrainment layer or capping inversion layer (between 0.7 and 1 of the PBL depth). Four main external factors determine the PBL depth and its mean vertical structure: (1) the free atmosphere wind speed; (2) the surface heat (more exactly buoyancy) balance; (3) the free atmosphere density stratification; (4) the free atmosphere vertical wind shear or baroclinicity. In fluid dynamics, the baroclinity (sometimes called baroclinicity) is a measure of the stratification in a fluid. ...


Principal types

Convective planetary boundary layer
(CBL, see also convection) is the PBL where positive buoyancy flux at the surface creates a thermal instability and thus generates additional or even major turbulence. The CBL is typical in tropical and mid-latitudes during daytime. Solar heating assisted by the heat realised from the water vapor condensation could create so strong convective turbulence that the CBL comprises the entire troposphere up to 10 km to 18 km (Intertropical convergence zone).
Stably stratified planetary boundary layer
(SBL) is the PBL where negative buoyancy flux at the surface damps the turbulence. The SBL is solely driven by the wind shear turbulence and hence the SBL cannot exist without the free atmosphere wind. The SBL is typical in nighttime at all locations and even in daytime in places where the earth's surface is colder than the air above. The SBL plays a particularly important role in high latitudes where it is often prolonged (days to months), resulting in very cold air temperatures.

Physical laws and equations of motions, which govern the planetary boundary layer dynamics and microphysics, are strongly non-linear and considerably influenced by properties of the earth's surface and evolution of the processes in the free atmosphere. To deal with this complicity, the whole array of turbulence modelling has been proposed. However, they are often not accurate enough to met practical requests. Significant improvements are expected from application of a large eddy simulation technique to problems related to the PBL. Convection in the most general terms refers to the internal movement of currents within fluids (i. ... The thunderstorms of the Intertropical Convergence Zone form a line across the eastern Pacific Ocean. ... Large eddy simulation (LES) is a numerical technique used to solve the partial differential equations governing turbulent fluid flow. ...


Perhaps the most important processes, which are critically dependent on the correct representation of the PBL in the atmosperic models (Atmospheric Model Intercomparison Project), are turbulent transport of moisture (evapotranspiration) and pollutants (air pollutants). Clouds in the boundary layer influence trade winds, the hydrological cycle, and energy exchange. Atmospheric Model Intercomparison Project (AMIP) is a standard experimental protocol for global atmospheric general circulation models (AGCMs). ... Evapotranspiration (ET) is the sum of evaporation and plant transpiration. ... Air pollution is a chemical, particulate matter, or biological agent that modifies the natural characteristics of the atmosphere. ... For other uses, see Cloud (disambiguation). ... The trade winds are a pattern of wind that are found in bands around the Earths equatorial region. ... The water cycle is known scientifically as the hydrologic cycle. ...


See also

In physics and fluid mechanics, a boundary layer is that layer of fluid in the immediate vicinity of a bounding surface. ... In fluid dynamics, turbulence or turbulent flow is a flow regime characterized by chaotic, stochastic property changes. ... Cirrus uncinus ice crystal plumes showing high level wind shear, with changes in wind speed and direction. ... Atmospheric physics is the application of physics to the study of the atmosphere. ... Atmospheric sciences is an umbrella term for the study of the atmosphere, its processes, the effects other systems have on the atmosphere, and the effects of the atmosphere on these other systems. ... Cloud to ground Lightning in the global atmospheric electrical circuit. ...

References

  1. ^ Wizelius, Tore (2007). Developing Wind Power Projects. London: Earthscan Publications Ltd, p. 40. ISBN 1844072622. “The relation between wind speed and height is called the wind profile or wind gradient.” 
  2. ^ a b Brown, G. (2001). Sun, Wind & Light. New York: Wiley, p. 18. ISBN 0471348775. 
  3. ^ Dalgliesh, W. A. and D. W. Boyd (1962-04-01). "CBD-28. Wind on Buildings". “Flow near the surface encounters small obstacles that change the wind speed and introduce random vertical and horizontal velocity components at right angles to the main direction of flow.” 
  4. ^ Hadlock, Charles (1998). Mathematical Modeling in the Environment. Washington: Mathematical Association of America. ISBN 088385709X. 
  5. ^ a b Lal, R. (2005). Encyclopedia of Soil Science. New York: Marcel Dekker, p. 618. ISBN 0849350530. 
  6. ^ Oke, T. (1987). Boundary Layer Climates. London: Methuen, p. 54. ISBN 0415043190. “Therefore the vertical gradient of mean wind speed (dū/dz) is greatest over smooth terrain, and least over rough surfaces.” 
  7. ^ a b Crawley, Stanley (1993). Steel Buildings. New York: Wiley, p. 272. ISBN 0471842982. 
  8. ^ Lubosny, Zbigniew (2003). Wind Turbine Operation in Electric Power Systems : Advanced Modeling. Berlin: Springer, p. 17. ISBN 354040340X. 
  9. ^ Harrison, Roy (1999). Understanding Our Environment. Cambridge: Royal Society of Chemistry, p. 11. ISBN 0854045848. 
  10. ^ a b Thompson, Russell (1998). Atmospheric Processes and Systems. New York: Routledge, pp. 102-103. ISBN 0415171458. 
  11. ^ Gupta, Ajaya (1993). Guidelines for Design of Low-Rise Buildings Subjected to Lateral Forces. Boca Raton: CRC Press, p. 49. ISBN 0849389690. 
  12. ^ Stoltman, Joseph (2005). International Perspectives on Natural Disasters: Occurrence, Mitigation, and Consequences. Berlin: Springer, 73. ISBN 1402028504. 
  13. ^ Chen, Wai-Fah (1997). Handbook of Structural Engineering. Boca Raton: CRC Press, p. 12-50. ISBN 0849326745. 
  14. ^ Ghosal, M. (2005). "7.8.5 Vertical Wind Speed Gradient", Renewable Energy Resources. City: Alpha Science International, Ltd, pp. 378-379. ISBN 9781842651254. 
  15. ^ Stull, Roland (1997). An Introduction to Boundary Layer Meteorology. Boston: Kluwer Academic Publishers, p. 442. ISBN 9027727686. “...both the wind gradient and the mean wind profile itself can usually be described diagnostically by the log wind profile.” 
  16. ^ Thuillier, R.H.; Lappe, U.O. (1964). "Wind and Temperature Profile Characteristics from Observations on a 1400 ft Tower". Journal of Applied Meteorology 3 (3): 299-306. DOI:< 10.1175/1520-0450(1964)003<. Retrieved on 2007-06-10. 
  17. ^ Mcilveen, J. (1992). Fundamentals of Weather and Climate. London: Chapman & Hall, p. 184. ISBN 0412411601. 
  18. ^ Burton, Tony (2001). Wind Energy Handbook. London: J. Wiley, p. 20. ISBN 0471489972. 
  19. ^ Köpp, F.; Schwiesow, R.L.; Werner, C. (01 1984). "Remote Measurements of Boundary-Layer Wind Profiles Using a CW Doppler Lidar". Journal of Applied Meteorology and Climatology 23 (1): p. 153. DOI:< 10.1175/1520-0450(1984)023<. Retrieved on 2007-06-09. 
  20. ^ Johansson, C.; Uppsala, S.; Smedman, A.S. (2002). "Does the height of the boundary layer influence the turbulence structure near the surface over the Baltic Sea?". 15th Conference on Boundary Layer and Turbulence, American Meteorological Society. 
  21. ^ Shao, Yaping (2000). Physics and Modelling of Wind Erosion. City: Kluwer Academic, p. 69. ISBN 9780792366577. 

Journal of Applied Meteorology and Climatology (formerly Journal of Applied Meteorology) is a publication of the American Meteorological Society. ... A digital object identifier (or DOI) is a standard for persistently identifying a piece of intellectual property on a digital network and associating it with related data, the metadata, in a structured extensible way. ... Year 2007 (MMVII) is the current year, a common year starting on Monday of the Gregorian calendar and the AD/CE era. ... is the 161st day of the year (162nd in leap years) in the Gregorian calendar. ... Journal of Applied Meteorology and Climatology (formerly Journal of Applied Meteorology) is a publication of the American Meteorological Society. ... A digital object identifier (or DOI) is a standard for persistently identifying a piece of intellectual property on a digital network and associating it with related data, the metadata, in a structured extensible way. ... Year 2007 (MMVII) is the current year, a common year starting on Monday of the Gregorian calendar and the AD/CE era. ... June 9 is the 160th day of the year in the Gregorian calendar (161st in leap years), with 205 days remaining. ... The American Meteorological Society promotes the development and dissemination of information and education on the atmospheric and related oceanic and hydrologic sciences and the advancement of their professional applications. ...

External links


  Results from FactBites:
 
Planetary boundary layer - Wikipedia, the free encyclopedia (684 words)
The planetary boundary layer (PBL) is an atmospheric layer where physical quantities (flow velocity, temperature, moisture etc) are considerably affected by rapid fluctuations (Turbulence) resulting from the flow interaction with the earth's surface.
Above the surface layer the PBL turbulence gradually dissipate (Dissipation) loosing it kinetic energy to friction as well as converting the kinetic to potential energy in a density stratified flow.
Physical laws and equations of motions, which govern the planetary boundary layer dynamics and microphysics, are strongly non-linear and considerably influenced by properties of the earth's surface and evolution of the processes in the free atmosphere.
The Planetary Boundary Layer (2334 words)
The boundary layer is directly influenced by the presence of the Earth's surface, responding to such forcings as frictional drag, solar heating, and evapotranspiration.
The PBL height is determined as the greater of these two heights: that predicted from Ekman theory or the convective height that depends on dry static energy in the vertical (Phillips, 1990).
Once the PBL height is determined, the profile of the coefficient of diffusivity is specified as a cubic function of the PBL height.
  More results at FactBites »


 

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