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South African Journal of Science

versión On-line ISSN 1996-7489

S. Afr. j. sci. vol.109 no.5-6 Pretoria ene. 2013

 

RESEARCH LETTER

 

Is the southern Benguela a significant regional sink of CO2?

 

 

Luke GregorI; Pedro M.S. MonteiroI, II

IDepartment of Oceanography, University of Cape Town, Cape Town, South Africa
IIOcean Systems and Climate Group, CSIR, Stellenbosch, South Africa

Correspondence

 

 


ABSTRACT

This study was undertaken to characterise the seasonal cycle of air-sea fluxes of carbon dioxide (CO2) in the southern Benguela upwelling system off the South African west coast. Samples were collected from six monthly cross-shelf cruises in the St. Helena Bay region during 2010. CO2 fluxes were calculated from pCO2 derived from total alkalinity and dissolved inorganic carbon and scatterometer-based winds. Notwithstanding that it is one of the most biologically productive eastern boundary upwelling systems in the global ocean, the southern Benguela was found to be a very small net annual CO2 sink of -1.4 ± 0.6 mol C/m2 per year (1.7 Mt C/year). Regional primary productivity was offset by nearly equal rates of sediment and sub-thermocline remineralisation flux of CO2, which is recirculated to surface waters by upwelling. The juxtaposition of the strong, narrow near-shore out-gassing region and the larger, weaker offshore sink resulted in the shelf area being a weak CO2 sink in all seasons but autumn (-5.8, 1.4 and -3.4 mmol C/m2 per day for summer, autumn and winter, respectively).

Keywords: southern Benguela; eastern boundary; carbon dioxide; CO2; remineralisation


 

 

Introduction

Over the last 200 years, atmospheric carbon dioxide (CO2) concentrations have risen by 40% as a result of anthropogenic emissions from fossil fuel combustion and land use changes.1 Nearly 50% of anthropogenic emissions has been taken up by the oceans,2 acting as a natural mitigation mechanism against greenhouse warming. Recent estimates have found that the global oceans take up -2.2 Gt C/year,3 but this amount excludes that of the continental margins, which are estimated to have an annual uptake of up to -0.36 Gt C/year.4 The continental margins could potentially play an important role as anthropogenic CO2 sinks on national or regional scales, especially in areas where a significant proportion of the primary productivity carbon is naturally exported to the open ocean.5

This potential role could be particularly important to South Africa, the 13th largest CO2 emitter (119 Mt C/year).6 Several natural ecosystems have been identified as possible CO2 mitigation mechanisms, the broader categories being the terrestrial and marine biospheres. It is estimated that indigenous terrestrial ecosystems would realistically sequester 1-12 Mt C/year and would be effective as an active sink for only 30 years.7 Marine ecosystems may offer a more sustainable natural sequestration alternative. In recent years, marine ecosystems have received increased interest in this area, and have been dubbed 'blue carbon sinks'.8 The potential of blue carbon sinks lies predominantly in the conservation and rehabilitation of estuarine ecosystems such as mangrove forests, seagrasses and salt marshes.8 Shelf ecosystems are considered modest sinks in comparison to the aforementioned, but given the extent of the South African coastline, shelf carbon sequestration could be significant on a national scale. The Benguela upwelling system, the region of interest in this study, is considered a highly productive eastern boundary upwelling system, with the potential of being a CO2 sink.9 A study on the drivers of the air-sea CO2 fluxes in the southern Benguela was undertaken to better understand this system and to provide insight to this system being a regional sink and the sensitivities thereof.

The southern Benguela makes up the majority of the South African west coast, extending from 30°S to 35°S. This eastern boundary upwelling system is a highly productive shelf ocean (with an average annual rate of 54 mmol C/m2 per day)10 driven by equatorward alongshore winds. Seasonality in the southern Benguela is driven by the meridional migration and intensification of the South Atlantic Anti-Cyclone (SAAC).11 The southernmost extent of the SAAC occurs during summer months, resulting in alongshore winds favourable to upwelling. Northward migration of the SAAC and the weakening of the low pressure trough over the sub-continent during winter weakens the intensity of upwelling winds and allows mid-latitude cyclones to pass further north, which strengthen downwelling conditions. This seasonal forcing results in changes to the physics, chemistry and biology of the southern Benguela upwelling system, and thus changes in CO2 flux.9

Previous studies on the air-sea CO2 fluxes of the Benguela have found the region to be an annual sink of -1.70 (in 1994 and 1995) and -2.02 Mt C/year in 2005.5,12 González-Dávila et al.13 reported large interannual variability in the Benguela south of 32°S during 2006 and 2007 (-1.17 and -3.24 mol C/m2 per year, respectively), where the region was reportedly a continuous sink. This study provides a mechanistic perspective on the seasonality of contemporary air-sea CO2 fluxes in the southern Benguela by analysis of the marine carbonate system and nutrients.

 

Methods

Water samples were collected for six months (January, April, May, June, August and September) during 2010 along the St. Helena Bay Monitoring Line (SHBML). A conductivity, temperature and depth rosette with General Oceanics-Niskin bottles was lowered to various depths at each of the 12 stations (Figure 1). Samples were analysed for dissolved inorganic carbon (DIC) and total alkalinity (TA) using a Versatile Instrument for the Determination of Titration Alkalinity and Total Carbon (VINDTA 3C) by Marianda (Kiel, Germany).14 The precision achieved for DIC and TA was ±3.7 ^mol/kg and 2.5 ^mol/kg, respectively. Partial pressure of CO2 (pCO2) was calculated from DIC and TA using dissociation constants by Dickson and Millero15. A propagation of error analysis of pCO2 resulted in- an error of ±20 ^atm. Nitrate, phosphate and silicate were collected and analysed using methods described by Grasshoff16.

 

 

Sea-air CO2 flux was calculated using:

where kw is the gas transfer velocity,17K0 is the solubility of CO2 in seawater18 and Δρϋϋ2 is the difference between oceanic and atmospheric pCO2. Atmospheric pCO2 was considered to be the same as that measured at Cape Point.6 The gas transfer velocity (kw) was calculated using the empirical parameterisation by Wanninkhof et al.17 and Atlas Cross-Calibrated Multi-Platform wind product (CCMP winds).19 The gas transfer velocity was calculated using daily averaged winds. The flux was calculated by interpolating ΔpCO2 over the entire year. Calculations of CO2 fluxes for the southern Benguela used an area of 104 000 km2.5

 

Results and discussion

The average seasonal cycle of CO2 fluxes (Figure 2) was calculated using the zonal averages. Summer (September - January) and winter (May -August) were CO2 sinks with fluxes of -5.8 and -3.4 mmol C/m2 per day, respectively (see Table 1 for summary). Autumn (February - April) was the only season where the flux was positive (1.4 mmol C/m2 per day), which means that the region was a CO2 source over this period. These estimates showed the same decreasing trend from summer to winter as that reported by Chen and Borges4, namely a decrease in uptake from -11.0 mmol C/m2 per day in summer to -5.5 mmol C/ m2 per day in winter (note that uptake is negative and outgassing is positive). The net annual flux estimate for the region was -1.4 ± 0.6 mol C/m2 per year - equivalent to the uptake of 1.8 ± 0.8 Mt C/year for 2010. The former value compares well with those reported in previous studies on the region (Table 1).5,12,13 A great deal of interannual variability was observed during 2006-2007 as a result of changes in upwelling intensity; however, the region remained a sink over the entire period.13 This finding is in contrast to those of this study, where autumn was found to be a CO2 source to the atmosphere. This difference could be a result of interannual variability or because the study by González-Dávila et al.13 was biased towards the offshore region, where waters were consistently a carbon sink (Figure 2).

 

 

The boundary between the offshore sink and nearshore source regions migrated considerably throughout 2010 (Figure 2). The extent of this boundary was determined by the relative magnitudes of primary productivity and remineralisation during the seasonal cycle as well as the cumulative intensity of seasonal upwelling. Remineralisation of organic matter occurred predominantly in bottom waters and sediments resulting in increased pCO2.20 A cross section of the SHBML (Figure 3) depicts the remineralisation of exported particulate organic matter to DIC in bottom waters. The idealised circulation depicted in this figure brings CO2-enriched water to the surface in the nearshore region, where surface processes such as primary productivity decrease the partial pressure of CO2. The balance between these two dominant counteracting processes (remineralisation and primary production) plays a first-order role in determining the CO2 flux with the atmosphere, but lower-order contributors to the marine carbonate system cannot be overlooked.

The contribution of the processes that alter the pCO2 was calculated by analysis of changes in nutrient, DIC and TA ratios and their impact on pCO2 changes (Table 2 and Figure 4). The two most dominant processes were primary production and remineralisation. The effect of primary production ranged between -98 and -28 µatm CO2/day and aerobic remineralisation between 39 and 95 µatm CO2/day. These processes are simple to understand as a large change in DIC by primary production or remineralisation leads to a proportional change in pCO2. This relationship is not true for the other processes where simultaneous increases or decreases of DIC or TA lead to a complex response of pCO2 - an increase in DIC leads to increased pCO2, whereas an increase in TA leads to a decrease in pCO2. It is then the ratio of change of DIC to TA, which is specific to each process, that determines the pCO2 (Table 2). Denitrification was marginal in summer and autumn contributing ca. 5.4 µatm CO2/day and negligible during winter. In contrast to denitrification, sulphate reduction led to decreased pCO2 (as a result of increased TA), with the most dominant contribution, reducing pCO2 by -11 ^atm CO2/day, occurring in autumn. Sulphate reduction during summer and winter (-5 CO2/day and -4 µatm CO2/day) contributed in the same order of magnitude to denitrification, mitigating the increased pCO2. Calcification, resulting in a decrease in TA, led to strong increases in surface pCO2 during autumn,21 equating to 50% of the DIC uptake by primary production. This proportion was significantly greater than that found in studies in the North Atlantic that reported significantly lower net community calcification than net community production (13%).22 Evidently, autumn biogeochemistry was dissimilar from the other seasons because of intensification of a seasonal sub-thermocline oxygen minimum zone.23 Reduced upwelling and mixing in autumn led to intense and persistent stratification, resulting in decreased ventilation of sub-thermocline waters. Aerobic remineralisation eventually depleted oxygen to a level where anaerobic remineralisation became viable. Anaerobic processes such as denitrification and calcification increased the pCO2, which was upwelled to surface waters.20 The resulting air-sea CO2 fluxes were low given the aerobic remineralisation fluxes (-27 ^atm CO2/day to 1 µatm CO2/day). However, it was the counteracting primary production that took up DIC and decreased pCO2 that resulted in the low CO2 fluxes.

 

 

 

 

Studies suggest that ocean-atmosphere heat fluxes, shelf width, wind stress variability and shelf boundary exchange mechanisms may be important in determining the direction and magnitude of flux.23-25 These factors explain the inconsistent CO2 flux results among eastern boundary current systems at similar latitudes, such as the Humboldt (-0.3 - 1.94 mol C/m2 per year)26, Californian (2.2 - 0.7 mol C/m2 per year)4 and Galician (-2.2 mol C/m-2 per year)4 as well as the difference between the two Benguela subsystems.12 The southern Benguela may export a higher proportion of its new production across the ocean-shelf boundary compared to its northern counterpart, where trapping of particular organic carbon in alongshore inshore sediment belts supports persistent anaerobic remineralisation.23 Widespread denitrification is more intense in the northern Benguela upwelling system, leading to nitrate deficits, thus resulting in the region being a CO2 source.20,24

Evidence from the southern and northern Benguela subsystems then agrees with the idealised notion that temperate shelf systems are sinks, while those at lower latitudes are sources.4 The exact mechanism that enhances shelf export in the southern Benguela is unclear, but the high eddy kinetic energy in this sector suggests that eddy-driven transport may be an important vector, as has been observed in the Californian upwelling system.27,28 Previous estimates of CO2 export across the shelf boundary are larger by an order of magnitude (7.2-39.0 Mt C/year) than the sea-air CO2 fluxes presented in this study, supporting a finding of offshore transport of CO2.29

Extrapolating the findings of this study to other coastal regions of South Africa should be done with caution. The southern coast bears resemblance to the west coast and is likely to also be a weak CO2 sink.30 The same does not hold for the subtropical east coast where a narrow shelf and river inputs present an entirely different physical setting.31 A separate study would have to be conducted on these regions to effectively determine whether the South African continental margins are a net sink or source of CO2.

 

Conclusion

The seasonality of air-sea CO2 flux and biogeochemical drivers of the marine carbonate system of the southern Benguela upwelling system were investigated. With the inclusion of the two previous estimates, the magnitude of CO2 flux ranges from -1.7 to -2.0 Mt C/year.5,12,13 The reason for this modest sink, in the context of high primary productivity rates, is that the net annual carbon uptake is balanced by the nearly equally large remineralised carbon fluxes from the sediments and sub-thermocline waters.

Now, more than ever, it is important to strengthen long-term observations of our coastal-shelf regions as reports of decreasing fish stocks in the southern Benguela reveal a changing ecosystem.9 The larger impacts of ocean acidification linked to increased anthropogenic CO2 emissions will increase the stresses on these overexploited stocks. Moreover, naturally elevated Revelle factors make this region particularly sensitive to increased atmospheric pCO2. Changing driving mechanisms (winds) and increasing atmospheric CO2, could alter this 'steady state' in the southern Benguela, enhancing the sink or source fluxes depending on which part of the carbon cycle or eddy driven shelf export is altered. The evolution of the dynamic carbon cycle of the southern Benguela region may also provide insight into future changes of ocean carbon chemistry in other comparable upwelling systems regions.

 

Acknowledgements

We thank Dr Howard Waldron for his support and co-supervision and the Departments of Environment (Ocean and Coasts Branch) and Agriculture and Fisheries for allowing the sampling of the St. Helena Bay Monitoring Line to be undertaken onboard their ships. We are thankful to the National Research Foundation for a studentship to L.G. and the Council for Scientific and Industrial Research for a Parliamentary Grant. This research was conducted as part of the Southern Ocean Carbon - Climate Observatory (SOCCO) programme.

Authors' contributions

L.G. wrote the manuscript based on work from his MSc dissertation. P.M.S.M. supervised the work and reviewed and edited the manuscript.

 

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Correspondence:
Luke Gregor
Department of Oceanography, University of Cape Town
Private Bag, Rondebosch 7700, South Africa
Email: lukegre@gmail.com

Received: 13 June 2012
Revised: 05 Dec. 2012
Accepted: 17 Jan. 2013

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