Effects of transfer processes on marine atmospheric boundary layer or Effects of boundary layer processes on air-sea exchange

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1 Effects of transfer processes on marine atmospheric boundary layer or Effects of boundary layer processes on air-sea exchange Ann-Sofi Smedman Uppsala University Uppsala, Sweden

2 Effect of transfer process on MABL Swell Long waves create form drag Ocean Upward momentum flux Quasi-frictional decoupling at the surface MABL Turbulence resembles free convection conditions

3 Effect of MABL process on air-sea exchange UVCN regime MABL Detached eddies impinging on the surface Ocean Increased C HN and C EN Increased small scale heat flux

4 In models air-sea exchange is described through Monin-Obukhov similarity theory a theory which is well tested over land but is it valid over the ocean?

5 What are the differences? Large heat capacity Small diurnal variation Roughness (waves) increasing with increasing wind speed

6 Long term measurements in the Baltic Sea 2 buoys (temp, wave height, dir. and CO 2 Footprint area Tower 30 m Temp and wind profiles 5 levels Turbulence 3 levels Humidity and CO 2 at 2 levels

7 Short term experiments with RV Aranda and ASIS buoy Turbulence, wind speed, temperature and wave parameters In the mean, excellent agreement between tower and ASIS

8 Data set from Agile experiment in lake Ontario A 15- m research vessel Agile was equipped to measure waves and turbulence with Sonic R2A Thermocouple Licor Wave staff array Measurements were performed at 7.8 m during two autumn periods

9 Growing sea (slow waves) Unstable stratification Monin-Obukhov similarity theory is valid but roughness length, z o, is a function of wave age 10 2 Growing sea z 0 /σ u * /c p

10 Swell (long waves traveling faster than the wind) and unstable stratification A quite different type of boundary layer develops

11 The swell driven BL is characterized by Small or positive momentum flux Low level jet M-O scaling does not hold The vertical extent can be global Turbulence spectra resemble free convection conditions Swell represents reverse atmospheric-ocean coupling

12 Small momentum flux Shearing stress F2 C p /U 8 =1.73 C3 C P /U 8 =1.61 C2 C p /U 8 =1.79 F1 C p /U 8 =4.66 height (m) 15 C1 C p /U 8 = u w (m 2 s 2 )

13 Positive momentum flux uw x 1000 Aircraft measurements positive uw Tower measurements

14 LES simulations Peter Sullivan

15 Low level jet Mean wind profiles Case C1 Case F1 C p /U 8 = 4.72 C p /U 8 = height (m) U (ms 1 )

16 35 30 Mean wind profiles Case C2 Case C3 Case F2 C p /U 8 = 1.79 C p /U 8 = 1.61 C p /U 8 = height (m) U (ms 1 )

17 The vertical extent is global 10 4 Pibal tracking LST 10 3 z (m) U (m/s)

18 Φ m calculated for five swell cases φ m = (1 15z/L) 1/4 for L= 30 m C1 Eq. C2 F1 F2 C3 20 height (m) C p /U 8 =4.7 5 C p /U 8 = φ m

19 Turbulent kinetic energy budget 0 = U u w z g T o 1 pw w e w θ ε ρ z z o P B T p T t D

20 Turbulent energy budget Growing sea Energy S(n) (m 2 s 1 ) Growing sea case n peak = 0.42 Hz Frequency n (Hz) 25 Growing sea 20 height (m) P B Tp Tt D TKE (m 2 s 3 ) x 10 3

21 35 30 Mean wind profiles Case C1 Case F1 C p /U 8 = 4.72 C p /U 8 = Case F1 height (m) Turbulent energy budget c p /U=4.7 Energy S(n) (m 2 s 1 ) n swell = 0.22 Hz U (ms 1 ) Frequency n (Hz) Case F height (m) Tp B P Tt ε TKE (m 2 s 3 ) x 10 4

22 height (m) Mean wind profiles Case C2 Case C3 Case F2 C p /U 8 = 1.79 C p /U 8 = 1.61 C p /U 8 = 1.73 Turbulent energy budget c p /U=1.6 Energy S(n)(m 2 s 1 ) Case C3 n swell = 0.22 Hz n min =0.35 Hz U (ms 1 ) Frequency n (Hz) 25 Case C3 20 height (m) P B Tt ε Tp TKE (m 2 s 3 ) x 10 3

23 ) 2 ' ' ' ' ( ' ' 1 2 θ + ε + + = v T p w q z w T g w u z U ' ' ) ( w u T z U p Tp = dz u T m U U z z m p = * ) (2.5 ) ( From the turbulence energy eq, The effect of T p can be isolated

24 35 30 F2 (based on numerical expressions for Tp) blue: measured U curve 25 red: measured U curve minus Tp/u * 2 20 height U (ms 1)

25 Heat fluxes All turbulent fluxes in models must be expressed as mean variables Stanton number Heat flux C H = w θ U( T Ts ) o Wind speed Air-sea temperature difference In the same way for latent heat, C E

26 Reduced to neutral stability Von Karman constant=0.4 C HN = 2 κ {ln( z / z0)}{ln( z / z0 T )} Roughness length Roughness length for temperature In the same way for latent heat, C EN

27 Heat fluxes, unstable stratification ΔT>3 o Traditional parametrization (COARE algorithm) is valid No variation with wave age Heat fluxes, stable stratification Low-level jets cause shear suppression leading to decreased fluxes

28 Heat fluxes, unstable stratification, very close to neutral Wind speed > 10 m/s and ΔT< 3 o Fluxes are underestimated with COARE algorithm

29 Unstable stratification -- horizontal rolls 10 1 T u w U T ns u,w (n)/u * 2 Φε 2/3 nst (n)/t * 2 Φε 1/3 ΦNT w f=nz/u

30 Unstable near neutral -- detached eddies ns u,w (n)/u * 2 Φε 2/3 nst (n)/t * 2 Φε 1/3 ΦNT T u w U T w f=nz/u

31 Normalized heat fluxes Norm. heat flux Östergarnsholm 0.25 L= 250 m L= 10 m 0.2 nco wt (n)/wt 0.15 L= 42 m L= 140 m f=nz/u

32 Heat flux from Östergarnsholm 3 x MIUU, L > 150m data2 R2, 1 m/s bins MIUU, L < 150m; 0.5<(Tw T10) <1.0K MIUU, L < 150m; 1.0 < (Tw T10) < 1.5K Platinum MIUU, L < 150m; sensor 1.5 < (Tw ( T10) o < ***) 2.0 K ΔT<3 o C HN Sonic temp U 10

33 Latent heat flux, Östergarnsholm ΔΤ<2 ο COARE

34 Agile heat flux x Sonic TC ΔT<3 o C HN ΔT> thermocouple 1 ΔT>3 sonic U 10

35 Agile latent heat flux 3 x 10 3 Agile Licor, ΔT< C EN Solid curves data from Östergarnsholm U (ms 1 )

36 Agile heat flux: (wt) TC -( wt) sonic 0.04 Comparison of heat fluxes, differences, Agile 94, w t TC w t S (m s 1 K) U (m s 1 ) 10

37 The unstable very close to neutral regime The UVCN regime is defined for ΔT<3 o and U>10m/s It is found both over land and sea in the lowest region (z<15 m) of the surface layer Small scale heat flux is a result of detached eddies originating from the upper part of the surface. This is in contrast to a convective surface layer ruled by horizontal rolls.

38 Frequency (%) of occurrence of UVCN conditions ERA-40 reanalysis

39 Increase (W/m 2 ) in latent heat flux with UVCN regime included ERA-40 reanalysis

40 Global mean values of the increase of heat fluxes with UVCN regime included Sensible heat flux= 0.8 W/m 2 Latent heat flux (evaporation)= 2.4 W/m 2 The effect of increased anthropogenic greenhouse gases (2006) on net radiation = 2.63±0.26 W/m 2

41 Conclusions Unstable stratification M-O similarity theory is only valid for growing waves During swell the MABL is characterized by Low-level jet (LLJ) at 5-10 m height Constant wind speed above LLJ Small or positive momentum flux varying with height Energy is transported from waves to atmosphere by pressure transport term T p

42 Mixed seas As soon as a small portion of the waves are travelling faster than the wind (mixed seas) MABL is slowly changing from an ordinary boundary layer to a swell dominated boundary layer and Monin-Obukhov similarity theory is not valid During stable stratification wave effects are small

43 Heat fluxes The dynamics of the MABL influence the air-sea exchange of sensible and latent heat. When the convective boundary layer is ruled by horizontal rolls the well known COARE algorithm is valid. When detached eddies originating from the upper part of the surface layer is present (UVCN regime) the heat fluxes are increased and the Φ h -function goes to zero

44 Why has not the UVCN regime been observed earlier? sonic temperature fails to measure temperature fluctuations correctly when σ T is small (high wind speed, small ΔT) data with small ΔT are often removed from the data set measurements are taken at heights above the UVCN layer.

45 Thanks to Ulf Högström, Erik Sahlee, Anna Rutgersson, Hans Bergström, Cecilia Johansson, MIUU Will Drennan, RSMAS, Miami, Kimmo Kahma and Heidi Pettersson, FMRI, Helsinki Phd-students: Andreas Karelid, Björn Carlsson, Maria Norman, Alvaro Semedo Former Phd-students: Cecilia Johansson Birgitta Källstrand, Anna Rutgersson, Anna Sjöblom, Xiaoli Guo Larsen

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