My watch list
my.chemeurope.com  

my.chemeurope.com

With an accout for my.chemeurope.com you can always see everything at a glance – and you can configure your own website and individual newsletter.

  • My watch list
  • My saved searches
  • My saved topics
  • My newsletter
Register free of charge
Login  
eng  
DeutschEnglishFrançaisEspañol

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.

Contents

Cause of surface wind gradient

See also: Wind shear, Wind gradient, Wind Engineering, 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]

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]

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]

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]

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]

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]

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.

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.

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.

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.

See also

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. American Meteorological Society. 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. 
 
This article is licensed under the GNU Free Documentation License. It uses material from the Wikipedia article "Planetary_boundary_layer". A list of authors is available in Wikipedia.
Your browser is not current. Microsoft Internet Explorer 6.0 does not support some functions on Chemie.DE