Deep flow and mixing in the Indian Ocean
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1 Deep flow and mixing in the Indian Ocean MacKinnon Pinkel Johnston
2 Deep Mixing: Southwest Indian Ocean Evidence of elevated turbulence above the Southwest Indian Ridge Kunze et al 06 (+ correction Dec 06) Estimates from Lowered ADCP measurements during WOCE I!
3 Possible sources of mixing above the SW Indian Ridge Egbert and Ray Tidal Generation Near-inertial Geneartion M. Alford Study Area Internal waves with 12.4 hour period Internal waves with 15 hour period (inertial period in souther ocean)
4 Deep Mixing: Southwest Indian Ocean South Africa NADW Madagascar LCDW Southwest Indian Ridge AABW J.A. MacKinnon (SIO) R. Pinkel (SIO) T.M.S. Johnston (SIO) G. Carter (UH) O. Sun (SIO) S. Nguyen (SIO) A. Lucas (SIO) T. Huussen (NOC) Dec 07 - Jan 08 R/V Revelle Net overturning rate poorly constrained (3-30 Sv) NSF / UC Ship Funds Donohue et al 03, van Aken et al 03, Toole and Warren 93, Reid 93, Bryden and Beal 01
5 Deep Mixing: Southwest Indian Ocean South Africa NADW Madagascar LCDW Southwest Indian Ridge AABW Net overturning rate poorly constrained (3-30 Sv) Atlantis II Fracture Zone J.A. MacKinnon (SIO) R. Pinkel (SIO) T.M.S. Johnston (SIO) G. Carter (UH) O. Sun (SIO) S. Nguyen (SIO) A. Lucas (SIO) T. Huussen (NOC) Dec 07 - Jan 08 R/V Revelle NSF / UC Ship Funds Donohue et al 03, van Aken et al 03, Toole and Warren 93, Reid 93, Bryden and Beal 01
6 Southwest Indian Ocean: Instruments 4-day time series Wave-powered wire-walker Freely drifting Profile to 500 meters C,T, P, U,V, Flourescence Pinkel Fast CTD 1000 meters in 5 minutes C,T, P, microconductivity
7 Southwest Indian Ocean: Instruments 50-day mooring deployments McLane Moored Profilers (WHOI mooring pool) Full depth (2 profilers each) C,T,P, U,V
8 Southwest Indian Ocean: Instruments Atlantis II Fracture Zone Lowered ADCP (Kunze et al 06, Polzin) 2 cross-trench sections 36 hour time series Generous loan by Kevin Speer (FSU) 300 khz RDI broadband Full depth (6000 meters) Velocity, density => shear, strain 8-m nominal resolution ~40 meter actual resolution
9 Strong northward transport of deep+bottom water Typical V(z) Water mass transport [Jackett & McDougall 97, Donohue & Toole 03] deep water γ kg m 3 bottom water γ kg m 3 LCDW AABW
10 Strong northward transport of deep+bottom water Depth-integrated transport ( ϒ > ) Net deep and bottom transport of 3 ± 2 Sv Compare to Sv basin-wide MOC (consistent with Johnson et al 98 Drijfhout and Naveira Garabato 08,)
11 Strong northward transport of deep+bottom water Depth-integrated transport ( ϒ > ) Net deep and bottom transport of 3 ± 2 Sv Compare to Sv basin-wide MOC (consistent with Johnson et al 98 Drijfhout and Naveira Garabato 08,) Flow is below bounding topography! S C N east ridge #!!!,-./0$1$% )!!! west ridge 2!!!!"#$%$&!' () * + (( * + (# * +
12 Time variability of Deep Jet Variability of northward velocity - & 15 hours M2 Harmonic fits of V(z) Internal tide beams in upper water column / '()*+"#",$ 0 Jan 12-15, J/kg 1 Dec 3, 2007 Deep jet oscillates at 15 hours 2 3!-.& - -.& -./ -.0!"#"$"%!&
13 Estimating turbulence - overturns Static instabilities in density. Thorpe Scale mixing estimate (Dillon 82) 0... K ρ =0.32 NL 2 T!120 /...!1!0!1,0 '()*+"#"&! '()*+"#"&!130!1/0!140!110 Lt = 33 m! ! !, -.!! "#"$%"&!! -/!5-0,-./0/! "#"$%"&!!,-./-!
14 Estimating turbulence - finestructure Vertical wavenumber spectra S 2 /N 2 Strain κ = 2 * 10-5 m 2 /s Garrett-Munk Estimate turbulent diffusivity (κ) by comparing shear/strain spectral levels to canonical Garrett-Munk internal-wave spectrum, based on wave-wave interaction theory (Gregg et al 03, Polzin, McComas and Muller)
15 Turbulence profiles Velocity Dissipation Diffusivity - Thorpe scale method & Shear/strain method / '()*+"#",$ what produces mixing? 3!-.& - -.& -./ -.0!"#"$"%!& &-!6 &-!7 &-!2 &-!1 &-!0!"#"4",5!& 8 "#"$ / "%!& &-!/ "
16 Mean jet shear not unstable - Velocity Shear Dissipation Diffusivity - & / 4 5(* & / / '()*+"#",$ / !-.& - -.& -./ -.0!"#"$"%!& &-!7 &-!8 &-!3 &-!2 &-!; &-!7 &-!2 &-!1 &-!0!"#"9",:!& < " "#"$ / "%!& &-!/ %!/ 3
17 Fine-structure shear elevated - Velocity Shear Dissipation Diffusivity - & / 4 5(* & / / 4 78 / '()*+"#",$ / / !-.& - -.& -./ -.0!"#"$"%!& &-!9 &-!: &-!3 &-!2 &-!= &-!9 &-!2 &-!1 &-!0!"#";",<!& > " "#"$ / "%!& &-!/ %!/ 3
18 Mixing away the deep salinity maximum Steady change in water properties as water flows north through fracture zone m 2! / " C m 1 Deep Water Bottom Water 4000 m S / psu
19 What mixes away the salinity maximum? 1) Vertical/diapycnal turbulent mixing S(z) t = κ 2 S z 2 S(z) t : observed change between southern and northern profiles : transit time through fracture zone ~ days
20 What mixes away the salinity maximum? 1) Vertical/diapycnal turbulent mixing. observed diffusivity S(z) t = κ 2 S z 2 needed S(z) t : observed change between southern and northern profiles : transit time through fracture zone ~ days ' Explanation for discrepancy: ()*+,"#"-$ % 0 / 1 longer transit time due to recirculation stronger mixing elsewhere in FZ than what we observed 2 '.!/ '.!0!! "#"$ % '.!% "&!' '.!'
21 What mixes the salinity maximum? 2) Lateral (isopycnal) stirring S t = κ H 2 S y m possible leakage of fresher Madagascar Basin water through gaps in the ridge 2! / " C Deep Water 3000 m variability in T-S time series Bottom Water 4000 m S / psu
22 Tidal beams in upper ocean U(z) cw/ccw energy diffusivity Downward propagating
23 Tidal beams: model results Princeton Ocean Model (G. Carter) Data Modeled tidal beams fill the domain Ridge corrugation close to tidal wavelength Enhanced upper ocean shear and turbulence along entire length of SW Indian Ridge?
24 Tidal beams: model data comparison (G. Carter) Model reproduces vertical structure and phase of tidal beam. Next step is use model to extrapolate observed mixing along the 1000 km long ridge
25 Aside: what happened to the inertial waves?? Egbert and Ray Tidal Generation Near-inertial Geneartion M. Alford Study Area Internal waves with 12.4 hour period Internal waves with 15 hour period (inertial period in souther ocean)
26 Aside: what happened to the inertial waves?? no26a1 (F x, F y ) = (<p u >, <p v >) Depth Integrated IW Energy Flux (W m 1 ) Y (km) Depth (m) W m 1 Eastward X (km) Actual average wind input during cruise period = 6 mw/m 2 (42-52 S) => ~5 kw/m
27 Aside: what happened to the inertial waves?? no26a1 (F x, F y ) = (<p u >, <p v >) Depth Integrated IW Energy Flux (W m 1 ) Mooring spectra Y (km) Depth (m) W m 1 Eastward X (km) Actual average wind input during cruise period = 6 mw/m 2 (42-52 S) => ~5 kw/m Low modes must dissipate in ~10 deg latitude. Surface/ bottom bounces? ACC fronts?
28 Conclusions - another example of patchy mixing Dissipation in upper 2500 m only (above ridge crests) is about 15 mw/m 2, similar to Egbert and Ray Extrapolating along entire SW Indian Ridge gives a rough total dissipation rate of 12 GW Deep mixing in series of fracture zones much larger Indian Ocean mixing concentrated in western half of basin, Drijfhout and Naveira Garabato 07 argue that this zonal mixing asymmetry significantly impacts basin-wide circulation patterns.
29 Consequences of patchy mixing Strong mixing may continue as bottom water flows north in concentrated boundary current (Donohue et al 03) Palmer et al 07: Modeled Indian Ocean overturning streamfunction South Africa Madagascar Constant κ = NADW LCDW AABW Bottom enhanced diffusivity
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