Bange, Hermann W.

Brandt, Peter

Dengler, Marcus

Fischer, Tim

Kock, Annette

Steinhoff, Tobias

English

OceanRep

Is air-sea interaction inhibited  in tropical upwelling systems ? Tim Fischer, Annette Kock,  Tobias Steinhoff, Marcus Dengler,  Hermann W. Bange, Peter Brandt NORDATLANTIK GROOM SOLAS Mid-Term Strategy Meeting 26.-28.11.2012  Maybe the more precise question is: Is air-sea gas exchange overestimated in tropical upwelling systems when using common gas exchange parametrizations?  This question is motivated by our efforts to quantify greenhouse gas emissions from upwelling systems and oxygen minimum zones.  The usual technique is measuring mixed layer concentrations and then use bulk formulae. The results depend critically on the used parametrization for the gas transfer velocity kw.  100cckW 10 m 5 m Outline  Indications that air-sea gas exchange might be lower than calculated:               1    N2O surface layer budget in Canary upwelling system            2    Productivity estimates in Canary upwelling system            3    Observed diurnal stratification of surface layer  Planned research Nov. 2012 to Feb. 2013, Meteor cruises off Peru.   Maybe the more precise question is: Is air-sea gas exchange overestimated in tropical upwelling systems when using common gas exchange parametrizations?  Indication 1 N2O budget discrepancy in Canary upwelling system [study of A. Kock et al. 2012]  After 3 campaigns in 2007/2008 measuring N2O and  diapycnal mixing: Define a mixed layer box for an N2O budget. Delta N2O parametrized from SST anomalies. ONkW 2Vertical mixing and advection Horizontal mixing and advection MLD Net gas flux Mauritania After 3 campaigns in 2007/2008 measuring N2O and  diapycnal mixing: Define a mixed layer box for an N2O budget. Delta N2O parametrized from SST anomalies. ONkW 2Vertical mixing and advection Horizontal mixing and advection MLD Net gas flux Mauritania depends critically on chosen parametrization Indication 1 N2O budget discrepancy in Canary upwelling system [study of A. Kock et al. 2012]  Comparing different parametrizations for gas transfer velocity kw: Parametrization  Liss and Merlivat (1986) Wanninkhof (1992) Nightingale (2000) Outgassing : supply  2.3 4 3.3 Indication 1 N2O budget discrepancy in Canary upwelling system [study of A. Kock et al. 2012]  Comparing different parametrizations for gas transfer velocity kw: Could the missing quantity be produced in the mixed layer? Parametrization  Liss and Merlivat (1986) Wanninkhof (1992) Nightingale (2000) Outgassing : supply  2.3 4 3.3 Required source term to close the budget (nmol/kg/a)  33 80 61 Maximum conceivable N2O production in Mauritanian mixed layer is  about 10 nmol/kg/a. Indication 1 N2O budget discrepancy in Canary upwelling system [study of A. Kock et al. 2012]  Comparing different parametrizations for gas transfer velocity kw: Could the missing quantity be produced in the mixed layer? Parametrization  Liss and Merlivat (1986) Wanninkhof (1992) Nightingale (2000) Tsai and Liu (2003) Tsai and Liu (2003) is particularly for the case of surface slicks / surfactants and takes into account their function as a gas exchange barrier. The investigated area was highly biologically productive during the sampling periods, so conditions for surfactants were favourable. Outgassing : supply  2.3 4 3.3 0.9 Required source term to close the budget (nmol/kg/a)  33 80 61 -1 Indication 1 N2O budget discrepancy in Canary upwelling system [study of A. Kock et al. 2012]  Indication 2 Estimating productivity with a triple gas approach [study by T. Steinhoff et al. 2012] After 3 campaigns in 2005 to 2010 measuring N2O, CO2 and O2 surface concentrations.  How is air-sea gas exchange involved ? Vertical exchange negligible, no N2O produced in mixed layer Upwelled water near coast. N2O and CO2 supersaturated. O2 undersaturated. Concentrations adjust to equilibrium Indication 2 Estimating productivity with a triple gas approach [study by T. Steinhoff et al. 2012] Assume a gas exchange parametrization. N2O assumed as inert now provides a time stamp for the sampled water parcels. N2O CO2 hypothetical observed time time concentration 0 0 Using the time stamp calculate a hypothetical CO2 concentration (as if CO2 were inert). The additional observed CO2 loss is interpreted as caused by Net Community Production (NCP). The inferred NCP is critically dependent on the choice of gas exchange parametrization. Indication 2 Estimating productivity with a triple gas approach [study by T. Steinhoff et al. 2012] Assume a gas exchange parametrization. N2O assumed as inert now provides a time stamp for the sampled water parcels. N2O O2 hypothetical observed time time concentration 0 0 Using the time stamp calculate a hypothetical O2 concentration (as if O2 were inert). NCP is further constrained by O2 observations and observed nitrate uptake. Again the most consistent picture appears using Tsai and Liu (2003). Indication 3 Diurnal shallow stratification  Intermezzo  Surfactants is one candidate to explain measurements in Canary upwelling system.  Another reason for reduced air-sea gas exchange could be the existence of gas concentration gradients in the „mixed layer“. We have no direct evidence for this yet.  But we often observe stratification in the uppermost meters of the water column in the tropics, particularly in upwelling regions. This stratification undergoes a diurnal cycle.  A simple model suggests that diurnal shallow stratification can lead to recognizable reductions of gas exchange. 3a       Concentration gradients may cause flux overestimation 10 m 1 m 10 cm 1 cm 1 mm 100 % 103 %  100103 cckW Gas saturation 10 m 1 m 10 cm 1 cm 1 mm 100 % 103 %  100103 cckW Gas saturation 3a       Concentration gradients may cause flux overestimation 10 m 1 m 10 cm 1 cm 1 mm 100 % 103 %  100101 cckW Gas saturation 3a       Concentration gradients may cause flux overestimation 3b     Glider data at   0 N  10 W  show diurnal temperature cycle temperature °C … which translates to a diurnal cycle in stratification N2 = 1e-4 0 – 2 h … which translates to a diurnal cycle in stratification 2 – 4 h … which translates to a diurnal cycle in stratification 4 – 6 h … which translates to a diurnal cycle in stratification 6 – 8 h … which translates to a diurnal cycle in stratification 8 – 10 h … which translates to a diurnal cycle in stratification 10 – 12 h … which translates to a diurnal cycle in stratification 12 – 14 h … which translates to a diurnal cycle in stratification 14 – 16 h … which translates to a diurnal cycle in stratification 16 – 18 h … which translates to a diurnal cycle in stratification 18 – 20 h … which translates to a diurnal cycle in stratification 20 – 22 h … which translates to a diurnal cycle in stratification 22 – 24 h … which translates to a diurnal cycle in stratification M. Dengler log10 (eps) 3b                 Glider based turbulence measurements e M. Dengler log10 (eps) e 3b                 Glider based turbulence measurements T ε 3b                    Average diurnal cycles at  0 N  10 W Also seen from PIRATA mooring data (Wenegrat, McPhaden, 2012). 2008/2009 on    0 N  23 W   „Upper ocean thermal stratification traps wind momentum in the near-surface, creating a diurnal jet and increasing shear, introducing a diurnal cycle into the […] eddy viscosity“ Diurnal cycle in near-surface temperature and shear 3b  X qq t1  t20 m 10 m 3c                      Could diurnal stratification affect gas flux calculation?    Simple model:   inert gas from below, subsurface temporarily stagnant. How much will the equilibrium concentration in the subsurface react?  X qq t1  t2t 24-t 0 m 10 m 3c                      Could diurnal stratification affect gas flux calculation?    Simple model:   inert gas from below, subsurface temporarily stagnant. How much will the equilibrium concentration in the subsurface react?  X h qq t1  t2t 24-t 0 m 10 m 3c                      Could diurnal stratification affect gas flux calculation?    Simple model:   inert gas from below, subsurface temporarily stagnant. How much will the equilibrium concentration in the subsurface react?  3c                Simple model:   example stationary  solution  X 6 h 18 h h = 0.1 m       t = 6 h       wind = 3 Bft 103 % 100 % X 6 h 18 h h = 0.1 m       t = 6 h       wind = 3 Bft 103 % 100 % This is the depth range we usually get our gas concentrations from. By Niskin bottles or underway sampling. 3c                Simple model:   example stationary  solution  X 6 h 18 h 24 h Reference: 101 % 103 % h = 0.1 m       t = 6 h       wind = 3 Bft 100 % 3c                Simple model:   example stationary  solution  101 % 103 % h = 0.1 m       t = 6 h       wind = 3 Bft 100 % The observed saturation would  overestimate the gas flux by a factor of 3.  100103 cckWobs  100101 cckWref 3c                Simple model:   example stationary  solution  1.5 2 3 5 3c        Model result:   Flux overestimation depending on t and h  t h Ship-based CTD profiles from 2008/2009 off Peru show a high percentage of stratification at 5 to 10m depth N2 in 5 to 10m depth: > 10-5 s-2 (comparable to main thermocline) < 10-5 s-2 undecided Callao 3c  Planned research for 4 Meteor cruises off Peru Nov. 2012  to  Feb. 2013 Peru EBUS is a good place to watch out for shallow stratification, gas concentration gradients, surface slicks.  This will be part of the research happening through Meteor cruises M90 to M93.  Particularly on cruise M91 starting Nov. 28, which is a SOPRAN contribution to the SOLAS Mid-Term Strategy Initiative. 4  Sampling the surface microlayer (SOPRAN, TP  A. Engel) Cunliffe et al. 2012 Sampling N2O, T, S, mixing in the upper 10m First 1 m with pump 1 m to 10 m with Niskin Planned research for Meteor cruises off Peru Nov. 2012  to  Feb. 2013 4  M 91 During M92 and M93  7 gliders circling in a 1x1degree area. CTD, oxygen, chlorophyll, turbidity.  1 or 2 gliders with turbulence „MicroRider“ Planned research for Meteor cruises off Peru Nov. 2012  to  Feb. 2013 4  Summary We found 2 promising candidates for causing reduced gas exchange:    - Surface active substances (surfactants)    - Diurnal stratification of the „mixed layer“   During cruises in the Peru upwelling in Nov. 2012 to Feb. 2013 we hope to obtain data that allows more insight, comprising:    - Shallow CTD data - Shallow gas concentration profiles - Shallow turbulence data - Surface microlayer sampling   References:  Kock, A., J. Schafstall, M. Dengler, P. Brandt, and H. W. Bange: Sea-to-air and diapycnal nitrous oxide fluxes in the eastern tropical North Atlantic Ocean, Biogeosciences, 9, 957-964, 2012  Steinhoff, T., H. W. Bange, A. Kock, D. W. R. Wallace, and A. Körtzinger: Biological productivity in the Mauritanian upwelling estimated with a triple gas approach, Biogeosciences Discuss., 9, 4853-4875, 2012  Tsai, W. T. and K. K. Liu: An assessment of the effect of sea surface surfactant on global atmosphere-ocean CO2-flux, J. Geophys. Res.-Oceans, 108, 2003  Wenegrat, J. and M. J. McPhaden: Near Surface Eddy Viscosity at 0°N, 23°W Inferred from ADCP and Wind Stress Data, Poster presented at Tropical Atlantic Variability Meeting/PIRATA-17 Meeting, 10.-15.9.12, Kiel, Germany  Cunliffe, M., A. Engel, S. Frka, B. Gasparovic, C. Guitart, J. C. Murrell, M. Salter, C. Stolle, R. Upstill-Goddard, and O. Wurl: Sea surface microlayers: A unified physicochemical and biological perspective of the air-ocean interface, Progr. Oceanogr., 2012, in press, available online 

Is air-sea interaction inhibited in tropical upwelling systems?

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