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is constant, close to 0.40. For incompressible and frictionless ("ideal") fluids, Baumert (2013) used
Kolmogorov's classical ideas on turbulence to derive ideal values of a number of relevant constants of turbulent motions, among them
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268:
372:
199:
403:
Baumert, H. Z. (2013). "Universal equations and constants of turbulent motion" Physica
Scripta T155 (2013) 014001 (12pp). Online at stacks.iop.org/PhysScr/T155/014001
168:
314:
In recent years the von Kármán constant has been subject to periodic scrutiny. Reviews (Foken, 2006; Hogstrom, 1988; Hogstrom, 1996) report values of
61:
406:
Baumert H. Z., Wessling B. (2016). "On turbulence in dilatant dispersions". Physica
Scripta 91(7):074003. DOI:10.1088/0031-8949/91/7/074003
470:
221:
330:
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Hogstrom U (1988). "Non-dimensional wind and temperature profiles in the atmospheric surface layer-a re-evaluation".
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law describing the distribution of the longitudinal velocity in the wall-normal direction of a turbulent
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475:
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Gaudio, R. Miglio, R. and Dey, S. (2010). "Nonuniversality of von Kármán’s κ in fluvial streams".
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from Oak Ridge
National Laboratory Distributed Active Archive Center, Oak Ridge, Tennessee, U.S.A.
300:, heat and moisture from the atmosphere to the land surface. It is considered to be a universal (
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411:"Land Surface Model (LSM 1.0) for Ecological, Hydrological, Atmospheric Studies. Model product"
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Hogstrom U (1996). "Review of some basic characteristics of the atmospheric surface layer".
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argued that the Kármán constant is however nonuniversal in flows over mobile sediment beds.
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430:, International Association for Hydraulic Research (IAHR), Vol. 48, No. 5, 658-663
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a list of physical constants used in the NCAR Community
Climate System Model
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between 0.35 and 0.42. The overall conclusion of over 18 studies is that
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117:{\displaystyle u={\frac {u_{\star }}{\kappa }}\ln {\frac {z}{z_{0}}},}
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http://www.ccsm.ucar.edu/models/ccsm3.0/cpl6/users_guide/node21.html
419:
Foken T. (2006). "50 years of the Monin-Obukhov similarity theory".
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263:{\displaystyle u_{\star }={\sqrt {\frac {\tau _{w}}{\rho }}},}
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above the boundary. The roughness height (also known as
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367:{\displaystyle \kappa =1/{\sqrt {2\pi }}\approx 0.399}
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is the von Kármán constant being typically 0.41, and
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284:The Kármán constant is often used in
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170:appears to go to zero. Further
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428:Journal of Hydraulic Research
215:at the boundary of the flow:
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471:Boundary layer meteorology
442:Boundary Layer Meteorology
435:Boundary-Layer Meteorology
421:Boundary-Layer Meteorology
194:{\displaystyle u_{\star }}
16:Constant in fluid dynamics
51:. The equation for such
39:constant involved in the
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409:Bonan, G. B. (2005).
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205:which depends on the
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413:. Available on-line
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307:Gaudio, Miglio and
286:turbulence modeling
33:Theodore von Kármán
25:von Kármán constant
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55:flow profiles is:
444:, Vol. 42, 55-78.
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163:{\displaystyle u}
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392:Log wind profile
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290:meteorology
41:logarithmic
476:Turbulence
465:Categories
398:References
277:the fluid
135:at height
45:fluid flow
359:≈
354:π
335:κ
304:≈ 0.40).
252:ρ
243:τ
231:⋆
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150:is where
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79:⋆
381:See also
298:momentum
279:density
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127:where
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273:with
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309:Dey
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19:In
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89:ln
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338:=
320:κ
316:κ
302:κ
275:ρ
258:,
247:w
236:=
227:u
212:w
210:τ
183:u
172:κ
158:u
147:0
145:z
137:z
129:u
112:,
105:0
101:z
97:z
75:u
69:=
66:u
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