Search results
Results from the WOW.Com Content Network
The inertial speed's equation only helps determine either the speed or the radius of curvature once the other is given. The trajectory resulting from this motion is also known as inertial circle. The balance-flow model gives no clue on the initial speed of an inertial circle, which needs to be triggered by some external perturbation.
The Sverdrup balance, or Sverdrup relation, is a theoretical relationship between the wind stress exerted on the surface of the open ocean and the vertically integrated meridional (north-south) transport of ocean water.
Hsu gives a simple formula for a gust factor (G ) for winds as a function of the exponent (p), above, where G is the ratio of the wind gust speed to baseline wind speed at a given height: [28] G = 1 + 2 p {\displaystyle G=1+2p}
When estimating wind loads on structures the terrains may be described as suburban or dense urban, for which the ranges are typically 0.1-0.5 m and 1-5 m respectively. [ 2 ] In order to estimate the mean wind speed at one height ( z 2 {\displaystyle {{z}_{2}}} ) based on that at another ( z 1 {\displaystyle {{z}_{1}}} ), the formula would be ...
The power coefficient [9] C P (= P/P wind) is the dimensionless ratio of the extractable power P to the kinetic power P wind available in the undistributed stream. [ citation needed ] It has a maximum value C P max = 16/27 = 0.593 (or 59.3%; however, coefficients of performance are usually expressed as a decimal, not a percentage).
The power law is often used in wind power assessments [4] [5] where wind speeds at the height of a turbine ( 50 metres) must be estimated from near surface wind observations (~10 metres), or where wind speed data at various heights must be adjusted to a standard height [6] prior to use.
Get AOL Mail for FREE! Manage your email like never before with travel, photo & document views. Personalize your inbox with themes & tabs. You've Got Mail!
The Rossby number is the ratio of inertial force to Coriolis force, terms | | / and in the Navier–Stokes equations respectively. [ 1 ] [ 2 ] It is commonly used in geophysical phenomena in the oceans and atmosphere , where it characterizes the importance of Coriolis accelerations arising from planetary rotation .