Last edited by Kazizragore

Saturday, August 1, 2020 | History

2 edition of **Dynamic instability of stratified shear flow in the upper equatorial Pacific** found in the catalog.

Dynamic instability of stratified shear flow in the upper equatorial Pacific

Chaojiao Sun

- 374 Want to read
- 7 Currently reading

Published
**1997**
.

Written in English

- Shear waves -- Mathematical models.,
- Turbulence -- Mathematical models.,
- Ocean waves -- Pacific Ocean.

**Edition Notes**

Statement | by Chaojiao Sun. |

The Physical Object | |
---|---|

Pagination | 79 leaves, bound : |

Number of Pages | 79 |

ID Numbers | |

Open Library | OL15488989M |

The greater vertical shear of the thermally balanced Asian–Pacific and Atlantic jets in winter makes them prone to hydrodynamic instability, which in the context of geostrophic flows is called baroclinic instability. Baroclinic instability produces transient disturbances on subweekly time scales. problem of non-parallel stratified shear flows of an inviscid, incompressible fluid and examine the effects of the inclusion of the cross-flow on the stability of shear flows. Interestingly, we can prove that two components of iflow to the disturbances.

Reset your password. If you have a user account, you will need to reset your password the next time you login. You will only need to do this once. On Stratified Shear Flow in Sea Straits of Arbitrary Cross Section. Jian Deng. Interestingly, the presence of topographic variation does not alter the necessary condition for instability (Richardson number) nor the bounds on unstable eigenvalues (the semi‐circle theorem). The former can be proved using a new technique introduced herein.

COVID Resources. Reliable information about the coronavirus (COVID) is available from the World Health Organization (current situation, international travel).Numerous and frequently-updated resource results are available from this ’s WebJunction has pulled together information and resources to assist library staff as they consider how to handle . Cambridge Core - Oceanography and Marine Science - Double-Diffusive Convection - by Timour Radko.

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Dynamic instability of stratified shear flow in the upper equatorial Pacific Chaojiao Sun, 1 William D. Smyth, and James N. Mourn College of Oceanic and Atmospheric Sciences, Oregon State University, Corvallis Abstract. The role of stratified shear instability in maintaining the deep cycle of turbulence immediately below the equatorial mixed layer is examined by means Cited by: Dynamic instability of stratified shear flow in the upper equatorial Pacific Article (PDF Available) in Journal of Geophysical Research: Oceans (C5), May with.

The role of stratified shear instability in maintaining the deep cycle of turbulence immediately below the equatorial mixed layer is examined by means of linear stability analysis. The Taylor-Goldstein equation is solved numerically, using observed currents and stratification from the Tropical Instability Wave Experiment (TIWE).Cited by: Dynamic instability of stratified shear flow in the upper equatorial Pac ific Author: Chaojiao Sun, William D.

Smyth, James N. Mourn Created Date: The advantage of the wave interaction approach is that it provides a physical interpretation to shear flow instability. This paper is largely intended to purvey the basics of this physical interpretation to the reader, while both reviewing and consolidating previous work on the by: Effects of the baroclinic torque on wave propagation normally neglected under the Boussinesq approximation is investigated here, with a special focus on the associated consequences for the mechanistic interpretation of shear instability arising from the interaction between a pair of vorticity-propagating waves.

To illustrate and elucidate the physical effects. stratified compressible parallel shear flows to two-dimensional normal mode disturbances and obtalned a semicircle instability region for the complex wave velocity of an unstable mode.

Later, Chimonas () obtained a sufficient condition for stability, namely, that the flow is. Dynamic instability of stratified shear flow in the upper equatorial Pacific. Geophys. the lower and upper boundaries in solving the T–G equation by conducting three controlled experiments to the hour flow: case A—moving the upper boundary (from z = m) to z Transient overturning compensation between Atlantic and Indo.

Shear-flow instability is due to the interaction of the flow with the channel walls (encountered also in single-phase Poiseuille flow, i.e., Tollmien-Schlichting waves), which leads to transition to turbulent flow in either of the phases for sufficiently large Reynolds number.

The evolution of stratified shear flows with multilayer density distributions is discussed briefly from a theoretical perspective, generalizing the results of Caulfield [J. Fluid Mech.()] to allow for distinct types of instability are predicted to occur according to linear theory.

In the laboratory, we measure the density profile and the velocity profile. Shear instability of a stratified flow is one of the most complicated but fascinating problems in modern hydrodynamics. General stability conditions derived by Miles and Howard were followed by a sequence of special solutions describing the Kelvin-Helmholtz (KH).

[3] Shear flow instability in the atmosphere and oceans has been studied extensively, beginning in the 19th century with analyses by Helmholtz and Kelvin of step discontinuities in the density and horizontal wind speed in unbounded atmospheres.

Examining superposed streams of homogeneous fluid, Taylor showed that neutral waves can exist only when the Richardson. Stability of Stratified Compressible Shear Flows M. SUBBIAH AND R. JAIN Department of Mathematics, Indian Institute of Technology, KanpurIndia Submitted by E.

Stanley Lee Received August 3, For stratified compressible shear flows, it is shown that the instability. In the shear stratified flow below the surface mixed layer in the central equatorial Pacific, energetic near-N (buoyancy frequency) internal waves and turbulence mixing were observed by.

Variations of Equatorial Shear, Stratiﬁcation, and Turbulence Within a Tropical Instability Wave Cycle Ryuichiro Inoue1, Ren‐Chieh Lien2, James N.

Moum3, Renellys C. Perez4, and Michael C. Gregg2 1Research and Development Center for Global Change, Japan Agency for Marine‐Earth Science and Technology, Yokosuka, Japan, 2Applied Physics Laboratory, University of. Duane E. Stevens, Francis X. Crum, in Encyclopedia of Physical Science and Technology (Third Edition), I.F.3 Other Vertical Coordinates.

Dynamic meteorology uses several other vertical coordinates for particular problems. Sigma coordinates, defined by the vertical coordinate σ = p/p s, where p s is the surface pressure, are useful when the height of the lower boundary. The stability of stratified shear flows which occur in oceanic overflows, wind-driven thermoclines, and atmospheric inversion layers is governed by the Richardson Number Ri, a non-dimensional balance between stabilizing stratification and destabilizing shear.

For a shear flow with velocity difference U, density difference ∆ρ and characteristic length H, one has Ri = g (∆ρ. For the instability problem of density stratified shear flows in sea straits with variable cross sections, a new semielliptical instability region is found.

Furthermore, the instability of the bounded shear layer is studied in two cases: (i) the density which takes two different constant values in two layers and (ii) the density which takes three different constant.

STABILITY OF STRATIFIED SHEAR FLOWS We have thus established the following: LEMMA 4. For the existence of an unstable mode, we must have THEOREM 1. The complex wave velocity c for any unstable mode must lie inside the semiellipse-type region, in the upper half plane given by.

This book presents a unique and comprehensive view of the fundamental dynamical and thermodynamic principles underlying the large circulations of the coupled ocean-atmosphere system Dynamics of The Tropical Atmosphere and Oceans provides a detailed description of macroscale tropical circulation systems such as the monsoon, the Hadley and Walker.

The results of a laboratory experiment designed to study turbulent entrainment at sheared density interfaces are described. A stratified shear layer, across which a velocity difference Δ U and buoyancy difference Δ b is imposed, separates a lighter upper turbulent layer of depth D from a quiescent, deep lower layer which is either homogeneous (two-layer case) or linearly stratified .A linear analysis is made of the stability of flows, stratified with respect to depth, of an ideal liquid of finite depth with a Helmholtz velocity profile.

Apart from a Kelvin-Helmholtz wave, additional unstable modes are also discovered. Analytical expressions are obtained for the neutral curve of these modes. Their nature is discussed.The base flow consists of an unstable stratified shear layer (Ri(g) shear layer (Ri(g) > ), whose shear and stratification are varied.

The unstable shear layer undergoes a Kelvin-Helmholtz shear instability that develops into billows.