Turbulence decay in stratified and homogeneous marine layers
A spectral approach is applied to shear-induced turbulence in stratified layers. A system of spectral equations for stationary balance of turbulent energy and temperature variances was deduced in the vicinity of the local shear scale L sub(U) =( epsilon /U sub(Z) super(3) )
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| Veröffentlicht in: | Dynamics of atmospheres and oceans 1996-01, Vol.23 (1-4), p.15-25 |
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| creator | Lozovatsky, Iossif D |
| description | A spectral approach is applied to shear-induced turbulence in stratified layers. A system of spectral equations for stationary balance of turbulent energy and temperature variances was deduced in the vicinity of the local shear scale L sub(U) =( epsilon /U sub(Z) super(3) ) |
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A system of spectral equations for stationary balance of turbulent energy and temperature variances was deduced in the vicinity of the local shear scale L sub(U) =( epsilon /U sub(Z) super(3) )<<SUPER . At wavenumbers between the inertial-convective (k super(-) <<SUPER and weak turbulence (k super(-) super(3) ) subranges, additional narrow spectral intervals--`production' subranges--may appear (E identical with k super(-) super(1) , E sub(T) identical with k super(-) super(2) ). The upper boundary of these subranges is determined as L sub(U) , and the lower boundaries as L sub(R) identical with ( epsilon /U sub(Z) N super(2) )<<SUPER and L sub(T) identical with ( epsilon /U sub(Z) ) super(-) <<SUPER . It is shown that the scale L sub(U) is a unique spectral scale that is uniform up to a constant value for every hydrophysical field. It appears that the spectral scale L sub(U) is equivalent to the Thorpe scale L sub(T) sub(h) for the active turbulence model. Therefore, if turbulent patches are generated in a background of permanent mean shear, a linear relation between temperature and mass diffusivities exists. In spectral terms, the fossil turbulence model corresponds to the regime of the Boldgiano-Obukhov buoyancy subrange (E identical with k super(-) <<SUPER , E sub(T) identical with k super(-) <<SUPER . During decay the buoyancy subrange is expanded to lower and higher wavenumbers. At lower wavenumbers the buoyancy subrange is bounded by L sub(*) sub(*) =3( chi <<SUPER /N<<SUPER , which is equivalent to the Thorpe scale L sub(R) sub(h) . In such a transition regime only, when the viscous dissipation rate is removed from the set of main turbulence parameters, the Thorpe scale does not correlate with the buoyancy scale L sub(N) identical with epsilon <<SUPER and fossil turbulence is realized. Oceanic turbulence measurements in the equatorial Pacific near Baker Island confirm the main ideas of the active and fossil turbulence models.]]></description><identifier>ISSN: 0377-0265</identifier><language>eng</language><ispartof>Dynamics of atmospheres and oceans, 1996-01, Vol.23 (1-4), p.15-25</ispartof><lds50>peer_reviewed</lds50><woscitedreferencessubscribed>false</woscitedreferencessubscribed></display><links><openurl>$$Topenurl_article</openurl><openurlfulltext>$$Topenurlfull_article</openurlfulltext><thumbnail>$$Tsyndetics_thumb_exl</thumbnail><link.rule.ids>314,776,780</link.rule.ids></links><search><creatorcontrib>Lozovatsky, Iossif D</creatorcontrib><title>Turbulence decay in stratified and homogeneous marine layers</title><title>Dynamics of atmospheres and oceans</title><description><![CDATA[A spectral approach is applied to shear-induced turbulence in stratified layers. A system of spectral equations for stationary balance of turbulent energy and temperature variances was deduced in the vicinity of the local shear scale L sub(U) =( epsilon /U sub(Z) super(3) )<<SUPER . At wavenumbers between the inertial-convective (k super(-) <<SUPER and weak turbulence (k super(-) super(3) ) subranges, additional narrow spectral intervals--`production' subranges--may appear (E identical with k super(-) super(1) , E sub(T) identical with k super(-) super(2) ). The upper boundary of these subranges is determined as L sub(U) , and the lower boundaries as L sub(R) identical with ( epsilon /U sub(Z) N super(2) )<<SUPER and L sub(T) identical with ( epsilon /U sub(Z) ) super(-) <<SUPER . It is shown that the scale L sub(U) is a unique spectral scale that is uniform up to a constant value for every hydrophysical field. It appears that the spectral scale L sub(U) is equivalent to the Thorpe scale L sub(T) sub(h) for the active turbulence model. Therefore, if turbulent patches are generated in a background of permanent mean shear, a linear relation between temperature and mass diffusivities exists. In spectral terms, the fossil turbulence model corresponds to the regime of the Boldgiano-Obukhov buoyancy subrange (E identical with k super(-) <<SUPER , E sub(T) identical with k super(-) <<SUPER . During decay the buoyancy subrange is expanded to lower and higher wavenumbers. At lower wavenumbers the buoyancy subrange is bounded by L sub(*) sub(*) =3( chi <<SUPER /N<<SUPER , which is equivalent to the Thorpe scale L sub(R) sub(h) . In such a transition regime only, when the viscous dissipation rate is removed from the set of main turbulence parameters, the Thorpe scale does not correlate with the buoyancy scale L sub(N) identical with epsilon <<SUPER and fossil turbulence is realized. Oceanic turbulence measurements in the equatorial Pacific near Baker Island confirm the main ideas of the active and fossil turbulence models.]]></description><issn>0377-0265</issn><fulltext>true</fulltext><rsrctype>article</rsrctype><creationdate>1996</creationdate><recordtype>article</recordtype><recordid>eNqNy00OgjAQQOEuNBF_7jArdySDBcHEndF4APZkhEFrSqsduuD2JsYDuHqb781UgrosU9zti4VaijwRMSuqQ6KOdQy3aNm1DB23NIFxIGOg0fSGOyDXwcMP_s6OfRQYKBjHYGniIGs178kKb35dqe3lXJ-u6Sv4d2QZm8FIy9bSd26yKit1jqj_hh-M1zqd</recordid><startdate>19960101</startdate><enddate>19960101</enddate><creator>Lozovatsky, Iossif D</creator><scope>7TG</scope><scope>KL.</scope></search><sort><creationdate>19960101</creationdate><title>Turbulence decay in stratified and homogeneous marine layers</title><author>Lozovatsky, Iossif D</author></sort><facets><frbrtype>5</frbrtype><frbrgroupid>cdi_FETCH-proquest_miscellaneous_181734003</frbrgroupid><rsrctype>articles</rsrctype><prefilter>articles</prefilter><language>eng</language><creationdate>1996</creationdate><toplevel>peer_reviewed</toplevel><toplevel>online_resources</toplevel><creatorcontrib>Lozovatsky, Iossif D</creatorcontrib><collection>Meteorological & Geoastrophysical Abstracts</collection><collection>Meteorological & Geoastrophysical Abstracts - Academic</collection><jtitle>Dynamics of atmospheres and oceans</jtitle></facets><delivery><delcategory>Remote Search Resource</delcategory><fulltext>fulltext</fulltext></delivery><addata><au>Lozovatsky, Iossif D</au><format>journal</format><genre>article</genre><ristype>JOUR</ristype><atitle>Turbulence decay in stratified and homogeneous marine layers</atitle><jtitle>Dynamics of atmospheres and oceans</jtitle><date>1996-01-01</date><risdate>1996</risdate><volume>23</volume><issue>1-4</issue><spage>15</spage><epage>25</epage><pages>15-25</pages><issn>0377-0265</issn><abstract><![CDATA[A spectral approach is applied to shear-induced turbulence in stratified layers. A system of spectral equations for stationary balance of turbulent energy and temperature variances was deduced in the vicinity of the local shear scale L sub(U) =( epsilon /U sub(Z) super(3) )<<SUPER . At wavenumbers between the inertial-convective (k super(-) <<SUPER and weak turbulence (k super(-) super(3) ) subranges, additional narrow spectral intervals--`production' subranges--may appear (E identical with k super(-) super(1) , E sub(T) identical with k super(-) super(2) ). The upper boundary of these subranges is determined as L sub(U) , and the lower boundaries as L sub(R) identical with ( epsilon /U sub(Z) N super(2) )<<SUPER and L sub(T) identical with ( epsilon /U sub(Z) ) super(-) <<SUPER . It is shown that the scale L sub(U) is a unique spectral scale that is uniform up to a constant value for every hydrophysical field. It appears that the spectral scale L sub(U) is equivalent to the Thorpe scale L sub(T) sub(h) for the active turbulence model. Therefore, if turbulent patches are generated in a background of permanent mean shear, a linear relation between temperature and mass diffusivities exists. In spectral terms, the fossil turbulence model corresponds to the regime of the Boldgiano-Obukhov buoyancy subrange (E identical with k super(-) <<SUPER , E sub(T) identical with k super(-) <<SUPER . During decay the buoyancy subrange is expanded to lower and higher wavenumbers. At lower wavenumbers the buoyancy subrange is bounded by L sub(*) sub(*) =3( chi <<SUPER /N<<SUPER , which is equivalent to the Thorpe scale L sub(R) sub(h) . In such a transition regime only, when the viscous dissipation rate is removed from the set of main turbulence parameters, the Thorpe scale does not correlate with the buoyancy scale L sub(N) identical with epsilon <<SUPER and fossil turbulence is realized. Oceanic turbulence measurements in the equatorial Pacific near Baker Island confirm the main ideas of the active and fossil turbulence models.]]></abstract></addata></record> |
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| source | Elsevier ScienceDirect Journals Complete |
| title | Turbulence decay in stratified and homogeneous marine layers |
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