Remember Me
Or use your Academic/Social account:


Or use your Academic/Social account:


You have just completed your registration at OpenAire.

Before you can login to the site, you will need to activate your account. An e-mail will be sent to you with the proper instructions.


Please note that this site is currently undergoing Beta testing.
Any new content you create is not guaranteed to be present to the final version of the site upon release.

Thank you for your patience,
OpenAire Dev Team.

Close This Message


Verify Password:
Verify E-mail:
*All Fields Are Required.
Please Verify You Are Human:
fbtwitterlinkedinvimeoflicker grey 14rssslideshare1
Planchon, F.; Cavagna, Anne-Julie; Cardinal, Damien; André, Luc; Dehairs, Frank (2013)
Publisher: European Geosciences Union
Languages: English
Types: Article
Subjects: DOAJ:Earth and Environmental Sciences, DOAJ:Earth Sciences, QH540-549.5, QE1-996.5, Evolution, QH501-531, Geology, DOAJ:Biology, Life, QH301-705.5, Q, Ecology, [PHYS.PHYS.PHYS-GEO-PH] Physics [physics]/Physics [physics]/Geophysics [physics.geo-ph], Science, DOAJ:Biology and Life Sciences, QH359-425, Biology (General)
During the Bonus-GoodHope (BGH) expedition (Jan–Mar 2008) we studied the water column distribution of total <sup>234</sup>Th and biogenic particulate Ba (Ba<sub><i>xs</i></sub>) in the Atlantic sector of the Southern Ocean. The objective was to assess the export flux of particulate organic carbon (POC) from the surface to the mesopelagic twilight zone along a section between the Cape Basin and Weddell Gyre. Export production of POC was estimated from steady state and non steady state export fluxes of <sup>234</sup>Th which were converted into POC fluxes, using the POC/<sup>234</sup>Th ratio of large (>53 μm) suspended particles, collected via in-situ pumps. Deficits in <sup>234</sup>Th activities were observed at all stations from the surface to the bottom of the mixed-layer. <sup>234</sup>Th export fluxes from the upper 100 m ranged from 496 &plusmn; 57 dpm m<sup>−2</sup> d<sup>−1</sup> to 1195 &plusmn; 120 dpm m<sup>−2</sup> d<sup>−1</sup> for the steady state model and from 149 &plusmn; 18 dpm m<sup>−2</sup> d<sup>−1</sup> to 1217 &plusmn; 146 dpm m<sup>−2</sup> d<sup>−1</sup> for the non steady state model calculated for a time window of 15 to 22 days preceding the timing of the present cruise. The POC/<sup>234</sup>Th<sub>p</sub> ratio of large, potentially sinking particles (>53 μm), was observed to increase with latitude, from 1.9 &plusmn; 0.2 μmol dpm<sup>−1</sup> and 1.7 &plusmn; 0.3 μmol dpm<sup>−1</sup> in the Subtropical Zone (STZ) and Subantarctic Zone (SAZ), respectively, to 3.0 &plusmn; 0.2 μmol dpm<sup>−1</sup> in the Polar Front Zone (PFZ), 4.8 &plusmn; 1.9 μmol dpm<sup>−1</sup> at the Southern Antarctic Circumpolar Current Front (SACCF) to 4.1 &plusmn; 1.7 μmol dpm<sup>−1</sup> in the northern Weddell Gyre, in line with an increasing contribution of larger cell diatoms. Steady state and non steady state POC export from the upper 100 m ranged from 0.9 &plusmn; 0.2 mmolC m<sup>−2</sup> d<sup>−1</sup> to 5.1 &plusmn; 2.1 mmolC m<sup>−2</sup> d<sup>−1</sup> and from 0.3 &plusmn; 0.0 mmolC m<sup>−2</sup> d<sup>−1</sup> to 4.9 &plusmn; 3.2 mmolC m<sup>−2</sup> d<sup>−1</sup>, respectively. From the SAZ to the SACCF, non steady state POC export production represented only 15 to 54 % of the steady state POC flux, suggesting that the intensity of export had decreased over time partly due to the fact that regenerated-production based communities of small-sized phytoplankton became predominant. In contrast, for the HNLC area south of the SACCF, we found an excellent agreement between the two modeling approaches indicating that surface POC export remained rather constant there. Estimated POC export represented between 6 to 54 % of the potential export as represented by new production, indicating that export efficiency was particularly low throughout the studied area, except close to the SACCF. <br><br> Below the export layer, in the mesopelagic zone, <sup>234</sup>Th activities generally reached equilibrium with <sup>238</sup>U, but sometimes were in large excess relative to <sup>238</sup>U (<sup>234</sup>Th/<sup>238</sup>U ratio>1.1), reflecting intense remineralisation/disaggregation of <sup>234</sup>Th-bearing particles. The accumulation of excess <sup>234</sup>Th in the 100–600 m depth interval ranged from 458 &plusmn; 55 dpm m<sup>−2</sup> d<sup>−1</sup> to 3068 &plusmn; 368 dpm m<sup>−2</sup> d<sup>−1</sup>. Using POC to <sup>234</sup>Th ratio of sinking particles, we converted this <sup>234</sup>Th flux into a POC remineralisation flux, which ranged between 0.9 to 9.2 mmolC m<sup>−2</sup> d<sup>−1</sup>. Mesopelagic remineralisation was also evidenced by Ba<sub><i>xs</i></sub> inventories which are related to bacterial degradation of sinking material and offer a means to quantify the flux of respired C. Highest biogenic particulate Ba (Ba<sub><i>xs</i></sub>) contents were generally observed in the 200–400 m depth interval with values reaching up to >1000 pM in the northern PFZ. Depth weighted average mesopelagic Ba<sub><i>xs</i></sub> (meso-Ba<sub><i>xs</i></sub>) was high in the PFZ and low in the northernmost (STZ-SAZ) and the southernmost (SACCF-AZ-WG) parts of the BGH section; conversion into respired C flux yielded a range of –0.23 to 6.4 mmolC m<sup>−2</sup> d<sup>−1</sup>. Excluding two outliers, we found a significant positive correlation for mesopelagic waters between POC remineralisation estimated from meso-Ba<sub><i>xs</i></sub> and from <sup>234</sup>Th excess (<i>R</i><sup>2</sup> = 0.73). Our results indicate that POC export production in this area of the Southern Ocean was strongly attenuated in the mesopelagic waters due to remineralisation, a process which thus appears to strongly impact on longer term bathypelagic zone sequestration of POC.