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Academic literature on the topic 'Trapped lee waves'

Author: Grafiati
Published: 10 December 2022
Last updated: 28 January 2023

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Journal articles on the topic "Trapped lee waves"

1

Tutiš, V. "Trapped lee waves: A special analytical solution." Meteorology and Atmospheric Physics 50, no. 4 (December 1992): 189–95. http://dx.doi.org/10.1007/bf01026016.

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2

Hills, Matthew O. G., and Dale R. Durran. "Nonstationary Trapped Lee Waves Generated by the Passage of an Isolated Jet." Journal of the Atmospheric Sciences 69, no. 10 (May 22, 2012): 3040–59. http://dx.doi.org/10.1175/jas-d-12-047.1.

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Abstract The behavior of nonstationary trapped lee waves in a nonsteady background flow is studied using idealized three-dimensional (3D) numerical simulations. Trapped waves are forced by the passage of an isolated, synoptic-scale barotropic jet over a mountain ridge of finite length. Trapped waves generated within this environment differ significantly in their behavior compared with waves in the more commonly studied two-dimensional (2D) steady flow. After the peak zonal flow has crossed the terrain, two disparate regions form within the mature wave train: 1) upwind of the jet maximum, trapped waves increase their wavelength and tend to untrap and decay, whereas 2) downwind of the jet maximum, wavelengths shorten and waves remain trapped. Waves start to untrap approximately 100 km downwind of the ridge top, and the region of untrapping expands downwind with time as the jet progresses, while waves downstream of the jet maximum persist. Wentzel–Kramers–Brillouin (WKB) ray tracing shows that spatial gradients in the mean flow are the key factor responsible for these behaviors. An example of real-world waves evolving similarly to the modeled waves is presented. As expected, trapped waves forced by steady 2D and horizontally uniform unsteady 3D flows decay downstream because of leakage of wave energy into the stratosphere. Surprisingly, the downstream decay of lee waves is inhibited by the presence of a stratosphere in the isolated-jet simulations. Also unexpected is that the initial trapped wavelength increases quasi-linearly throughout the event, despite the large-scale forcing at the ridge crest being symmetric in time about the midpoint of the isolated-jet simulation.
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Teixeira, Miguel A. C., José Luis Argaín, and Pedro M. A. Miranda. "Orographic Drag Associated with Lee Waves Trapped at an Inversion." Journal of the Atmospheric Sciences 70, no. 9 (September 1, 2013): 2930–47. http://dx.doi.org/10.1175/jas-d-12-0350.1.

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Abstract The drag produced by 2D orographic gravity waves trapped at a temperature inversion and waves propagating in the stably stratified layer existing above are explicitly calculated using linear theory, for a two-layer atmosphere with neutral static stability near the surface, mimicking a well-mixed boundary layer. For realistic values of the flow parameters, trapped-lee-wave drag, which is given by a closed analytical expression, is comparable to propagating-wave drag, especially in moderately to strongly nonhydrostatic conditions. In resonant flow, both drag components substantially exceed the single-layer hydrostatic drag estimate used in most parameterization schemes. Both drag components are optimally amplified for a relatively low-level inversion and Froude numbers Fr ≈ 1. While propagating-wave drag is maximized for approximately hydrostatic flow, trapped-lee-wave drag is maximized for l2a = O(1) (where l2 is the Scorer parameter in the stable layer and a is the mountain width). This roughly happens when the horizontal scale of trapped lee waves matches that of the mountain slope. The drag behavior as a function of Fr for l2H = 0.5 (where H is the inversion height) and different values of l2a shows good agreement with numerical simulations. Regions of parameter space with high trapped-lee-wave drag correlate reasonably well with those where lee-wave rotors were found to occur in previous nonlinear numerical simulations including frictional effects. This suggests that trapped-lee-wave drag, besides giving a relevant contribution to low-level drag exerted on the atmosphere, may also be useful to diagnose lee-rotor formation.
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Broutman, Dave, Jun Ma, Stephen D. Eckermann, and John Lindeman. "Fourier-Ray Modeling of Transient Trapped Lee Waves." Monthly Weather Review 134, no. 10 (October 1, 2006): 2849–56. http://dx.doi.org/10.1175/mwr3232.1.

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Abstract The Fourier-ray method involves ray tracing in a Fourier-transform domain. The ray solutions are then Fourier synthesized to produce a spatial solution. Here previous steady-state developments of the Fourier-ray method are extended to include a transient source of mountain waves. The method is illustrated with an initial value problem in which the background flow is started abruptly from rest and then maintained at steady velocity. The resulting wave transience is modeled in a simple way. All rays that radiate from the mountain, including the initial rays, are assigned the full amplitude of the longtime steady-state solution. Time dependence comes in through the changing position of the initial rays. This is sufficient to account for wave transience in a test case, as demonstrated by comparison with simulations from a mesoscale numerical model.
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Metz, Johnathan J., Dale R. Durran, and Peter N. Blossey. "Unusual Trapped Mountain Lee Waves with Deep Vertical Penetration and Significant Stratospheric Amplitude." Journal of the Atmospheric Sciences 77, no. 2 (January 30, 2020): 633–46. http://dx.doi.org/10.1175/jas-d-19-0093.1.

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Abstract Simulations of the weather over the South Island of New Zealand on 28 July 2014 reveal unusual wave activity in the stratosphere. A series of short-wavelength perturbations resembling trapped lee waves were located downstream of the topography, but these waves were in the stratosphere, and their crests were oriented north–south, in contrast to both the northeast–southwest orientation of the spine of the Southern Alps and the crests of trapped waves present in the lower troposphere. Vertical cross sections through these waves show a nodal structure consistent with that of a higher-order trapped-wave mode. Eigenmode solutions to the vertical structure equation for two-dimensional, linear, Boussinesq waves were obtained for a horizontally homogeneous sounding representative of the 28 July case. These solutions include higher-order modes having large amplitude in the stratosphere that are supported by just the zonal wind component. Two of these higher-order modes correspond to trapped waves that develop in an idealized numerical simulation of the 28 July 2014 case. These higher-order modes are trapped by very strong westerly winds in the midstratosphere and are triggered by north–south-oriented features in the subrange-scale topography. In contrast, the stratospheric cross-mountain wind component is too weak to trap similar high-order modes with crest-parallel orientation.
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6

Ralph, F. Martin, Paul J. Neiman, Teddie L. Keller, David Levinson, and Len Fedor. "Observations, Simulations, and Analysis of Nonstationary Trapped Lee Waves." Journal of the Atmospheric Sciences 54, no. 10 (May 1997): 1308–33. http://dx.doi.org/10.1175/1520-0469(1997)054<1308:osaaon>2.0.co;2.

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7

Lott, François. "A New Theory for Downslope Windstorms and Trapped Mountain Waves." Journal of the Atmospheric Sciences 73, no. 9 (August 22, 2016): 3585–97. http://dx.doi.org/10.1175/jas-d-15-0342.1.

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Abstract Linear mountain gravity waves forced by a nonlinear surface boundary condition are derived for a background wind that is null at the surface and increases smoothly to reach a constant value aloft and for a constant buoyancy frequency. In this configuration, the mountain waves have a critical level just below the surface that is dynamically controlled by the surface and minimum Richardson number J. When the flow is very stable , and when the depth over which dissipations act is smaller than the mountain height, this critical-level dynamics easily produces large downslope winds and foehns. The downslope winds are more intense when the stability increases and much less pronounced when it decreases (when J goes below 1). In contrast, the trapped lee waves are very small when the flow is very stable, start to appear when , and can become pure trapped waves (e.g., not decaying downstream) when the flow is unstable (for ). For the trapped waves, these results are explained by the fact that the critical level absorbs the gravity waves downstream of the ridge when , while absorption decreases when J approaches 0.25. Pure trapped lee waves follow that when the absorption can become null in the nondissipative limit. In the background-flow profiles analyzed, the pure trapped lee waves also correspond to neutral modes of Kelvin–Helmholtz instability. The validity of the linear approximation used is tested a posteriori by evaluating the relative amplitude of the neglected nonlinear terms.
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Li, Liye, and Yi-Leng Chen. "Numerical Simulations of Two Trapped Mountain Lee Waves Downstream of Oahu." Journal of Applied Meteorology and Climatology 56, no. 5 (May 2017): 1305–24. http://dx.doi.org/10.1175/jamc-d-15-0341.1.

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AbstractTwo trapped lee-wave events dominated by the transverse mode downstream of the island of Oahu in Hawaii—27 January 2010 and 24 January 2003—are simulated using the Weather Research Forecasting (WRF) Model with a horizontal grid size of 1 km in conjunction with the analyses of soundings, weather maps, and satellite images. The common factors for the occurrences of these transverse trapped mountain-wave events are 1) Froude number [Fr = U/(Nh)] > 1, where U is the upstream speed of the cross-barrier flow, N is stability, and h is the mountain height; 2) insufficient convective available potential energy for the air parcel to become positively buoyant after being lifted to the top of the stable trade wind inversion layer; and 3) increasing cross-barrier wind speed with respect to height through the stable inversion layer, satisfying Scorer’s criteria between the inversion layer and the layer aloft. Within the inversion layer, where the Scorer parameter has a maximum, the wave amplitudes are the greatest. The two trapped mountain waves in winter occurred under strong prefrontal stably stratified southwesterly flow. On the other islands in Hawaii, where the mountaintops are below the base of the inversion, transverse trapped lee waves can occur under similar large-scale settings if the mountain height is lower than U/N. The high-spatial-and-temporal-resolution WRF Model successfully simulates the onset, development, and dissipation of these two events. Sensitivity tests for the 27 January 2010 case are performed with reduced relative humidity (RH). With a lower RH and less-significant latent heating, trapped lee waves have smaller amplitudes and shorter wavelengths.
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Jiang, Qingfang, James D. Doyle, Shouping Wang, and Ronald B. Smith. "On Boundary Layer Separation in the Lee of Mesoscale Topography." Journal of the Atmospheric Sciences 64, no. 2 (February 1, 2007): 401–20. http://dx.doi.org/10.1175/jas3848.1.

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Abstract The onset of boundary layer separation (BLS) forced by gravity waves in the lee of mesoscale topography is investigated based on a series of numerical simulations and analytical formulations. It is demonstrated that BLS forced by trapped waves is governed by a normalized ratio of the vertical velocity maximum to the surface wind speed; other factors such as the mountain height, mountain slope, or the leeside speedup factor are less relevant. The onset of BLS is sensitive to the surface sensible heat flux—a positive heat flux tends to increase the surface wind speed through enhancing the vertical momentum mixing and accordingly inhibits the occurrence of BLS, and a negative heat flux does the opposite. The wave forcing required to cause BLS decreases with an increase of the aerodynamical roughness zo; a larger zo generates larger surface stress and weaker surface winds and therefore promotes BLS. In addition, BLS shows some sensitivity to the terrain geometry, which modulates the wave characteristics. For a wider ridge, a higher mountain is required to generate trapped waves with a wave amplitude comparable to that generated by a lower but narrower ridge. The stronger hydrostatic waves associated with the wider and higher ridge play only a minor role in the onset of BLS. It has been demonstrated that although hydrostatic waves generally do not directly induce BLS, undular bores may form associated with wave breaking in the lower troposphere, which in turn induce BLS. In addition, BLS could occur underneath undular jump heads or associate with trapped waves downstream of a jump head in the presence of a low-level inversion.
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10

Reeder, Michael J., Neil Adams, and Todd P. Lane. "Radiosonde observations of partially trapped lee waves over Tasmania, Australia." Journal of Geophysical Research: Atmospheres 104, no. D14 (July 1999): 16719–27. http://dx.doi.org/10.1029/1999jd900038.

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Book chapters on the topic "Trapped lee waves"

1

Reames, Donald V. "Distinguishing the Sources." In Solar Energetic Particles, 49–69. Cham: Springer International Publishing, 2021. http://dx.doi.org/10.1007/978-3-030-66402-2_3.

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AbstractOur discussion of history has covered many of the observations that have led to the ideas of acceleration by shock waves or by magnetic reconnection in gradual and impulsive solar energetic particle (SEP) events, respectively. We now present other compelling observations, including onset timing, SEP-shock correlations, injection time profiles, high-energy spectral knees, e/p ratios, and intensity dropouts caused by a compact source, that have helped clarify these acceleration mechanisms and sources. However, some of the newest evidence now comes from source-plasma temperatures. In this and the next two chapters, we will find that impulsive events come from solar active regions at ≈ 3 MK, controlling ionization states Q, hence A/Q, and, in most gradual events, shocks accelerate ambient coronal material from ≤1.6 MK. When SEPs are trapped on closed loops they supply the energy for flares. In addition to helping to define their own origin, SEPs also probe the structure of the interplanetary magnetic field.
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Adam, John A. "Atmospheric Waves." In Rays, Waves, and Scattering. Princeton University Press, 2017. http://dx.doi.org/10.23943/princeton/9780691148373.003.0014.

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This chapter deals with the underlying mathematics of atmospheric waves. Gravity waves occur between any stable layers of fluids that differ in density. When the fluid boundary is disturbed, buoyancy forces try to restore the equilibrium. The fluid returns to its original shape and overshoots before oscillations finally set in that propagate as waves. Internal gravity or buoyancy waves are often observed in the stable density layering of the upper atmosphere. The chapter first describes the linearized equations governing atmospheric waves before introducing a mathematical model of lee/mountain waves over an isolated mountain ridge, focusing on the basic equations and solutions, trapped lee waves, and billow clouds. It also considers wind shear, Howard's semicircle theorem, and the Taylor–Goldstein equation.
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