Changeset 333 for branches

Timestamp:

06/05/13 11:49:39 (11 years ago)

Author:

pinsard

Message:

new ref thanks to ads

Location:

branches/bibliolocean

Files:

• data/biblioref.bib (modified) (29 diffs)
• src/define_authors.sh (modified) (2 diffs)

branches/bibliolocean/data/biblioref.bib

@@ -4 +4 @@
 @PREAMBLE{"Bibliographie du LOCEAN"}
 
+@inproceedings{RobinsonEtourneauEtAl:AGU:2011,
+    hal_id = {hal-00830476},
+  loceanbibid = {01949},
+  loceanaffectation = {cnrs},
+  loceanteam = {paleoproxus},
+  timestamp = {20120605},
+ads={2011AGUFM.B41B0214R},
+    url = {http://hal.archives-ouvertes.fr/hal-00830476},
+    title = {{Evidence for oceanic oxygen depletion in the face of cooling in the early Pleistocene}},
+    author = {Robinson, R. S. and Etourneau, Johan and Martinez, P. and Schneider, R. R.},
+    abstract = {{Future climate change is predicted to significantly impact ocean circulation and, potentially, to reduce ocean oxygenation. Paradoxically, the transition from the warm Pliocene, often held as an analog for a future, warmer Earth, to the cool Pleistocene appears to accompany a decrease in intermediate water oxygenation. The Plio-Pleistocene cooling begins with the onset of major Northern Hemisphere glaciation, around 3.0-2.7 million years ago (Ma). High latitude cooling and extension of the polar ice caps led to cooling of the deep ocean and shoaling of the thermocline. The transition culminated in the cooling of the whole surface ocean and establishment of strong zonal and meridional atmospheric circulation from 2.0 Ma. A compilation of high-resolution nitrogen isotope records from the eastern equatorial Pacific, North Pacific, and the Arabian Sea and a global multi-site survey, indicates that regional intensification of oxygen minimum zones (OMZs) and expansion of water column denitrification accompanied the cooling and circulation changes at \~2.0 Ma. Large-scale open ocean suboxia intensified with the inception of a modern polar frontal system, despite lower temperatures and thus higher initial oxygen contents of the mode waters themselves. This likely reflects the increased importance of aged mode waters as the principle conduit of nutrients and oxygen to the OMZs. These results stress how climate-related changes in circulation may complicate our ability to predict ocean biogeochemical changes on a changing Earth.}},
+    keywords = {[0469] BIOGEOSCIENCES / Nitrogen cycling;[0470] BIOGEOSCIENCES / Nutrients and nutrient cycling;[4845] OCEANOGRAPHY: BIOLOGICAL AND CHEMICAL / Nutrients and nutrient cycling;[4912] PALEOCEANOGRAPHY / Biogeochemical cycles;processes;and modeling;},
+    language = {Anglais},
+    affiliation = {Laboratoire d'Oc{\'e}anographie et du Climat : Exp{\'e}rimentations et Approches Num{\'e}riques - LOCEAN},
+    booktitle = {{American Geophysical Union, Fall Meeting 2011}},
+    pages = {0214},
+date={2011-12-05/2011-12-09},
+    address = {San Francisco, CA, {\'E}tats-Unis},
+    journal = {American Geophysical Union},
+    volume = {41},
+    audience = {internationale},
+    year = {2011},
+    month = dec,
+}
+
+@article{EtourneauCollinsEtAl:CPD:2013,
+  loceanbibid = {01948},
+  loceanaffectation = {cnrs},
+  loceanteam = {paleoproxus},
+  timestamp = {20120605},
+    hal_id = {hal-00830470},
+ads={2013CliPD...9....1E},
+    title = {{Holocene climate variations in the western Antarctic Peninsula: evidence for sea ice extent predominantly controlled by insolation and ENSO variability changes}},
+    author = {Etourneau, Johan and Collins, L. G. and Willmott, V. and Kim, J. H. and Barbara, L. and Leventer, A. and Schouten, S. and Sinninghe Damst{\'e}, J. S. and Bianchini, A. and Klein, V. and Crosta, X. and Mass{\'e}, G.},
+    abstract = {{The West Antarctic ice sheet is particularly sensitive to global warming and its evolution and impact on global climate over the next few decades remains difficult to predict. In this context, investigating past sea ice conditions around Antarctica is of primary importance. Here, we document changes in sea ice presence, upper water column temperatures (0-200 m) and primary productivity over the last 9000 yr BP (before present) in the western Antarctic Peninsula (WAP) margin from a sedimentary core collected in the Palmer Deep basin. Employing a multi-proxy approach, we derived new Holocene records of sea ice conditions and upper water column temperatures, based on the combination of two biomarkers proxies (highly branched isoprenoid (HBI) alkenes for sea ice and TEXL86 for temperature) and micropaleontological data (diatom assemblages). The early Holocene (9000-7000 yr BP) was characterized by a cooling phase with a short sea ice season. During the mid-Holocene (\~ 7000-3000 yr BP), local climate evolved towards slightly colder conditions and a prominent extension of the sea ice season occurred, promoting a favorable environment for intensive diatom growth. The late Holocene (the last \~ 3000 yr) was characterized by more variable temperatures and increased sea ice presence, accompanied by reduced local primary productivity likely in response to a shorter growing season compared to the early or mid-Holocene. The stepwise increase in annual sea ice duration over the last 7000 yr might have been influenced by decreasing mean annual and spring insolation despite an increasing summer insolation. We postulate that in addition to precessional changes in insolation, seasonal variability, via changes in the strength of the circumpolar Westerlies and upwelling activity, was further amplified by the increasing frequency/amplitude of El Ni{\\~n}o-Southern Oscillation (ENSO). However, between 4000 and 2100 yr BP, the lack of correlation between ENSO and climate variability in the WAP suggests that other climatic factors might have been more important in controlling WAP climate at this time.}},
+    language = {Anglais},
+    affiliation = {Laboratoire d'Oc{\'e}anographie et du Climat : Exp{\'e}rimentations et Approches Num{\'e}riques - LOCEAN , Environnements et Pal{\'e}oenvironnements OC{\'e}aniques - EPOC},
+    pages = {1-41},
+    journal = {Climate of the Past Discussions},
+    volume = {9},
+    audience = {internationale},
+    doi = {10.5194/CPD-9-1-2013},
+    year = {2013},
+    month = jan,
+}
+
+
+@article{Etourneau:RobinsonEtAl:BD:2013,
+  loceanbibid = {01947},
+  loceanaffectation = {cnrs},
+  loceanteam = {paleoproxus},
+  timestamp = {20120605},
+ ads={2013BGD....10.5535E},
+    hal_id = {hal-00830464},
+    url = {http://hal.archives-ouvertes.fr/hal-00830464},
+    title = {{Equatorial Pacific peak in biological production regulated by nutrient and upwelling during the late Pliocene/early Pleistocene cooling}},
+    author = {Etourneau, Johan and Robinson, R. S. and Martinez, P. and Schneider, R.},
+    abstract = {{The largest increase in export production in the eastern Pacific of the last 5.3 Myr (million years) occurred between 2.2 and 1.6 Myr, a time of major climatic and oceanographic reorganization in the region. Here, we investigate the causes of this event using reconstructions of export production, nutrient supply and oceanic conditions across the Pliocene-Pleistocene in the eastern equatorial Pacific (EEP) for the last 3.2 Myr. Our results indicate that the export production peak corresponds to a cold interval marked by high nutrient supply relative to consumption, as revealed by the low bulk sedimentary 15N/14N ($\delta$15N) and alkenone-derived sea surface temperature (SST) values. This \~ 0.6 million years long episode of enhanced delivery of nutrients to the surface of the EEP was predominantly initiated through the upwelling of nutrient-enriched water sourced in high latitudes. In addition, this phenomenon was likely promoted by the regional intensification of upwelling in response to the development of intense Walker and Hadley atmospheric circulations. Increased nutrient consumption in the polar oceans and enhanced denitrification in the equatorial regions restrained nutrient supply and availability and terminated the high export production event.}},
+    language = {Anglais},
+    affiliation = {Laboratoire d'Oc{\'e}anographie et du Climat : Exp{\'e}rimentations et Approches Num{\'e}riques - LOCEAN , Climate and Environmental Physics [Bern]},
+    pages = {5535-5554},
+    journal = {Biogeosciences Discussions},
+    volume = {10},
+    audience = {internationale},
+    doi = {10.5194/BGD-10-5535-2013},
+    year = {2013},
+    month = mar,
+}
+
+@inproceedings{KimWillmottEtAl:EGU:2013,
+    hal_id = {hal-00830454},
+  loceanbibid = {01946},
+  loceanaffectation = {cnrs},
+  loceanteam = {paleoproxus},
+  timestamp = {20120605},
+    title = {{Application of the TEX86-L temperature proxy in the Southern Ocean}},
+    author = {Kim, Jung-Hyun and Willmott, Veronica and Etourneau, Johan and Crosta, Xavier and Massé, Guillaume and Bonnin, J{\'e}r{\^o}me and Schouten, Stefan and Sinninghe Damst{\'e}, Jaap S.},
+    abstract = {{The TEX86 (TetraEther indeX of tetraethers consisting of 86 carbon atoms, Schouten et al., 2002) paleothermometer was proposed based on the relative distribution of thaumarchaeotal lipids, i.e. isoprenoid glycerol dibiphytanyl glycerol tetraethers (GDGTs), and has been increasingly used to reconstruct past sea surface temperatures (SSTs). However, it appears that the TEX86 proxy might not be directly applicable for the polar oceans (Kim et al., 2008) and the use of a modified version of TEX86 with a logarithmic function which does not include the crenarchaeol regio-isomer (i.e. TEX86-L) seems to be a better option to reconstruct paleotemperatures in the Polar Oceans (Kim et al., 2010). More recently, a new calibration of TEX86-L with depth-integrated annual mean temperatures from 0 to 200 m water depth was also introduced with the calibration error of $\pm$2.8\degreC (Kim et al., 2012), since Thaumarchaeota are in low abundance in the Antarctic summer surface water (the \~0-45 m layer of low salinity water mass) but more abundant in winter in a \~45-105 m interval of cold, salty water (i.e. the summer remnant of the previous winter, surface-mixed layer) (Kalanetra et al., 2009). We applied the TEX86-L proxy and its 0-200 m calibration model on piston core MD03-2601 (66\degre03.07S; 138\degre33.43E; 746 m water depth) recovered from the eastern Antarctic continental margin and jumbo piston core 10 (JPC-10, 64\degre53'S, 64\degre12'W, 905 m water depth) obtained from the western Antarctic Peninsula. We also analyzed 19 sediment samples of ODP 1098 (64\degre51'S, 64\degre12'W, 1010 m water depth) drilled at the JPC-10 site for comparison with the record of Shevenell et al. (2011). The application of the TEX86-L on most recent sediments at core sites MD03-2601 and JPC-10 resulted in +4.0\degreC and +1.2\degreC temperature estimates, respectively, within the range reasonable of the present annual mean 0-200 m temperature at core sites considering the calibration error. TEX86-L-derived temperatures varied between +0\degreC and +4\degreC for the Holocene. The most striking features of the TEX86-L record were 1) a prominent increase in temperature centred at 6 kyr BP and 2) substantial temperature variability during the Late Holocene. The TEX86-L record from JPC-10 showed its maximum (>+3\degreC) at \~9,000 years BP. Following this peak, temperatures decreased to \~+1.5\degreC, until \~7,000 years BP. From \~7,000 to 4,200 years BP, temperatures slightly declined from +1.6 to +0.7\degreC, before reaching lowest values at \~3,000 years BP. The late Holocene was characterized by variable temperatures with a mean of +0.3\degreC. At around \~1,000 years BP, the temperature record exhibited a peak, with values approaching +2.5\degreC. Our new TEX86-L records from JPC-10 and ODP 1098 showed a consistent picture of temperature variation in Palmer Deep Basin. However, our results gave different temperature estimates in terms of amplitude and variations in comparison to the TEX86-SST values published by Shevenell et al. (2011). Our study also showed that TEX86-L derived temperatures at our core sites reflect a subsurface rather than a surface signal. Nevertheless, care has to be taken in interpreting the absolute values of TEX86-L derived reconstructions and relative changes in TEX86-L derived temperature can be viewed with more confidence. Kalanetra, K.M., Bano, N., and Hollibaugh, J.T.: Ammonia-oxidizing Archaea in the Arctic Ocean and Antarctic coastal waters, Environ. Microbiol., 11, 2434-2445, 2009. Kim, J.-H., Schouten, S., Hopmans, E.., Donner, B., and Sinninghe Damst{\'e}, J.S.: Global sediment core-top calibration of the TEX86 paleothermometer in the ocean, Geochim. Cosmochim. Acta, 72, 1154-1173, 2008. Kim, J.-H., van der Meer, J., Schouten, S., Helmke, P., Wilmott, V., Sangiorgi, F., Ko{\c c}, N., Hopmans, E.C., and SinningheDamst{\'e}, J.S.: New indices and calibrations derived from the distribution of creanarchaealisoprenoidtetraether lipids: Implications for past sea surface temperature reconstructions, Geochim. Cosmochim. Acta, 74, 4639-4654, 2010. Kim, J.-H., Crosta, X., Willmott, V., Renssen, H., Mass{\'e}, G., Bonnin, J., Helmke, P., Schouten, S., and Sinninghe Damst{\'e}, J.S.: Increase in Late Holocene subsurface temperature variability in East Antarctica, Geophys. Res. Lett., 39, L06705, doi:10.1029/2012GL051157, 2012. Schouten, S., Hopmans, E.C., Schefu{\ss}, E., and Sinninghe Damst{\'e}, J.S.: Distributional variations in marine crenarchaeotal membrane lipids: A new organic proxy for reconstructing ancient sea water temperatures? Earth Planet. Sci. Lett., 204, 265-274, 2002. Shevenell, A.E., Ingalls, A.E., Domack, E.W., and Kelly, C.: Holocene Southern Ocean surface temperature variability west of the Antarctic Peninsula, Nature, 470, 250-254, 2011.}},
+    language = {Anglais},
+    affiliation = {Laboratoire d'Oc{\'e}anographie et du Climat : Exp{\'e}rimentations et Approches Num{\'e}riques - LOCEAN , Department of Marine Organic Biogeochemistry , Department of Marine Biogeochemistry and Toxicology - NIOZ},
+    booktitle = {{EGU General Assembly 2013}},
+    pages = {9645},
+  date = {2013-04-07/2013-04-12},
+    address = {Vienne, Autriche},
+    volume = {15},
+    audience = {internationale},
+    year = {2013},
+    month = apr,
+ads={2013EGUGA..15.9645K},
+}
+
+@article{EtourneauEhlertEtAl:CPD:2012,
+    hal_id = {hal-00830442},
+  loceanbibid = {01945},
+  loceanaffectation = {cnrs},
+  loceanteam = {paleoproxus},
+  timestamp = {20120605},
+    title = {Contribution of changes in opal productivity and nutrient distribution in the coastal upwelling systems to late Pliocene/early Pleistocene climate cooling},
+    author = {Etourneau, Johan and Ehlert, C. and Frank, M. and Martinez, P. and Schneider, R.},
+    abstract = {{The global late Pliocene/early Pleistocene cooling (\~3.0-2.0 million years ago, Ma) concurred with extremely high diatom and biogenic opal production in most of the major coastal upwelling regions. This phenomenon was particularly pronounced in the Benguela Upwelling System (BUS), off Namibia, where it is known as the Matuyama Diatom Maximum (MDM). Our study focuses on a new diatom silicon isotope ($\delta$30Si) record covering the MDM in the BUS. Unexpectedly, the variations in $\delta$30Si signal follow biogenic opal content, whereby the highest $\delta$30Si values correspond to the highest biogenic opal content. We interpret the higher $\delta$30Si values during the MDM as a result of a stronger degree of silicate utilization in the surface waters caused by high productivity of mat-forming diatom species. This was most likely promoted by weak upwelling intensity dominating the BUS during the Plio/Pleistocene cooling combined with a large silicate supply derived from a strong Southern Ocean nutrient leakage responding to the expansion of Antarctic ice cover and the resulting stratification of the polar ocean 3.0-2.7 Ma ago. A similar scenario is hypothesized for other major coastal upwelling systems (e.g. off California) during this time interval, suggesting that the efficiency of the biological carbon pump was probably sufficiently enhanced in these regions during the MDM to have significantly increased the transport of atmospheric CO2 to the deep ocean. In addition, the coeval extension of the area of surface water stratification in both the Southern Ocean and the North Pacific, which decreased CO2 release to the atmosphere, led to further enhanced atmospheric CO2 drawn-down and thus contributed significantly to late Pliocene/early Pleistocene cooling.}},
+    language = {Anglais},
+    affiliation = {Laboratoire d'Oc{\'e}anographie et du Climat : Exp{\'e}rimentations et Approches Num{\'e}riques - LOCEAN},
+    pages = {669-694},
+    journal = {Climate of the Past Discussions},
+    volume = {8},
+    audience = {internationale},
+    doi = {10.5194/CPD-8-669-2012},
+    year = {2012},
+    month = mar,
+ads={2012CliPa...8.1435E},
+comment={20130605 : je (fp) ne connais pas la tutelle de Johan Etourneau},
+}
+
 @book{BerthierBoppEtAl:LP:2012,
   loceanbibid = {01944},
   loceanaffectation = {cnrs},
   loceanteam = {varclim, paleoproxus},
-  timestamp = {20120529,
+  timestamp = {20120529},
     hal_id = {hal-00801972},
-    title = {{En direct avec les scientifiques: 150 questions sur l'oc{\'e}an et le climat}},
+    booktitle = {{En direct avec les scientifiques: 150 questions sur l'oc{\'e}an et le climat}},
     author = {Berthier, {\'E}tienne and Bopp, Laurent and Charmasson, Sabine and Eymard, Laurence and Gemenne, Fran{\c c}ois and Goulletquer, Philippe and Ha-Duong, Minh and Hallegatte, St{\'e}phane and Le Cozannet, Gon{\'e}ri and Lefranc, Yann and Magnan, Alexandre and Masson-Delmotte, Val{\'e}rie and Meyssignac, Beno{\^\i}t and Racape, Virginie and Rochette, Julien and Waelbroeck, Claire},
     abstract = {{Ce livre est le t{\'e}moin vivant d un {\'e}change riche et unique entre 16 scientifiques et le grand public. Le changement climatique, en partie d{\^u} aux activit{\'e}s humaines, affecte l oc{\'e}an, r{\'e}gulateur important du climat. Les effets s observent d{\'e}j{\`a} {\`a} l'{\'e}chelle du monde : fonte des glaces continentales et oc{\'e}aniques, mont{\'e}e des eaux, acidification de l'oc{\'e}an... et leur impact sur les soci{\'e}t{\'e}s humaines s accentuera dans le demi-si{\`e}cle {\`a} venir. Il nous faut anticiper et pour nous adapter, mieux conna{\^\i}tre l oc{\'e}an et son r{\^o}le dans le climat, trouver des solutions applicables et acceptables par les populations. C est {\`a} cette relation {\'e}troite et fragile entre le climat, l oc{\'e}an et les hommes que s est int{\'e}ress{\'e}e l exposition qui a eu lieu {\`a} la Cit{\'e} des sciences entre le 6 avril 2011 et fin juin 2012. Exp{\'e}rience s{\'e}duisante, une borne permettait aux visiteurs de tous {\^a}ges de poser leurs questions, auxquelles 16 scientifiques ont r{\'e}pondu en fonction de leur domaine d expertise. " Comment se forment les vagues ? ", " Les ours polaires survivront-ils au r{\'e}chauffement climatique ? ", " C est quoi un tsunami ? ", " Venise sera-t-elle un jour sous l eau ? ", " L {\'e}volution actuelle du climat est-elle irr{\'e}versible ? ", " Les changements climatiques vont-ils provoquer des guerres ? ", " Quelle est la mer la plus pollu{\'e}e ? ", " Combien y a-t-il de CO2 dans la mer ? "... En tout, 150 questions et leurs r{\'e}ponses accessibles et ludiques. L ouvrage, mine d informations {\`a} la mise en pages graphique et a{\'e}r{\'e}e, a {\'e}t{\'e} con{\c c}u pour que le lecteur s y oriente le plus librement possible, s y prom{\`e}ne {\`a} son gr{\'e} selon ses propres interrogations, car chaque r{\'e}ponse peut se lire ind{\'e}pendamment des autres.}},
@@ -26 +139 @@
   loceanaffectation = {ird},
   loceanteam = {paleoproxus},
-  timestamp = {20120522,
+  timestamp = {20120522},
   title = {{Uso dos fen{\'o}is da lignina no estudo da mat{\'e}ria org{\^a}nica na V{\'a}rzea do Lago Grande Curu{\'a}i, Par{\'a} e no Lago do Ca{\c c}{\'o}, Maranh{\\~a}o, Brasil}},
     author = {Zocatelli, Renata and Cecanho, Fernanda and Amorin, Marcelo and Bernardes, Marcelo and Moreira-Turcq, Patricia and Turcq, Bruno and Sifeddine, Abdelfettah and Campello Cordeiro, Renato},
@@ -1911 +2024 @@
   loceanteam = {phybiocar,incas},
   phybiocartheme = {2},
-  timestamp = {20120419}
+  timestamp = {20120419},
   ads={2013DSR....88...23H},
   hal_id={hal-00824363},
@@ -1926 +2039 @@
   loceanbibid = {01467},
   loceanteam = {paleoproxus},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -1944 +2057 @@
   loceanbibid = {01465},
   loceanteam = {surf,varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -1959 +2072 @@
   loceanteam = {varclim},
   number = {numéro spécial},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -1978 +2091 @@
   loceanbibid = {01529},
   loceanteam = {varclim,nemo,phybiocar},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -1994 +2107 @@
   loceanbibid = {01750},
   loceanteam = {mmsa},
-  timestamp = {20121015}
+  timestamp = {20121015},
 }
 
@@ -2008 +2121 @@
   loceanbibid = {01748},
   loceanteam = {mmsa},
-  timestamp = {20121015}
+  timestamp = {20121015},
 }
 
@@ -2024 +2137 @@
   loceanbibid = {01749},
   loceanteam = {mmsa},
-  timestamp = {20121015}
+  timestamp = {20121015},
 }
 
@@ -2074 +2187 @@
   loceanbibid = {01921},
   loceanteam = {varclim},
-  timestamp = {20121219}
+  timestamp = {20121219},
 }
 
@@ -2089 +2202 @@
   loceanbibid = {01463},
   loceanteam = {varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2104 +2217 @@
   loceanbibid = {01524},
   loceanteam = {phybiocar,varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2118 +2231 @@
   loceanbibid = {01931},
   loceanteam = {phybiocar,caraus/snapo-co2},
-  timestamp = {20130204}
+  timestamp = {20130204},
 }
 
@@ -2136 +2249 @@
   loceanteam = {paleoproxus},
   publisher = {{B}lackwell {P}ublishing {L}td},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2150 +2263 @@
   loceanbibid = {01461},
   loceanteam = {varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2166 +2279 @@
   loceanbibid = {01522},
   loceanteam = {paleoproxus,phybiocar},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2181 +2294 @@
   loceanbibid = {01496},
   loceanteam = {phybiocar,varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2220 +2333 @@
   loceanbibid = {01312},
   loceanteam = {varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2234 +2347 @@
   loceanbibid = {01518},
   loceanteam = {varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2278 +2391 @@
   loceanbibid = {01812},
   loceanteam = {varclim},
-  timestamp = {20121014}
+  timestamp = {20121014},
 }
 
@@ -2322 +2435 @@
   loceanbibid = {01929},
   loceanteam = {paleoproxus},
-  timestamp = {20130102}
+  timestamp = {20130102},
 }
 
@@ -2336 +2449 @@
   loceanbibid = {01659},
   loceanteam = {varclim},
-  timestamp = {20120703}
+  timestamp = {20120703},
 }
 
@@ -2350 +2463 @@
   loceanbibid = {01517},
   loceanteam = {varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2367 +2480 @@
   loceanbibid = {01520},
   loceanteam = {phybiocar,varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2387 +2500 @@
   loceanteam = {surf},
   nationality = {F},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2433 +2546 @@
   loceanbibid = {01938},
   loceanteam = {varclim},
-  timestamp = {20130220}
+  timestamp = {20130220},
 }
 
@@ -2448 +2561 @@
   loceanbibid = {01459},
   loceanteam = {surf,varclim},
-  timestamp = {20120419}
+  timestamp = {20120419},
 }
 
@@ -2469 +2582 @@
   loceanbibid = {01731},
   loceanteam = {varclim},
-  timestamp = {20120810}
+  timestamp = {20120810},
 }
 

branches/bibliolocean/src/define_authors.sh

@@ -38 +38 @@
 #
 # 
+# - fplod 20130605T082059Z cratos.locean-ipsl.upmc.fr (Linux)
+#
+#   * add Johan Etourneau
 # - fplod 20130411T144800Z cratos.locean-ipsl.upmc.fr (Linux)
 #
@@ -517 +520 @@
 list_author_file[${iauthor}]="Taphanel_mariehelene"
 #
+iauthor=$(( ${iauthor} + 1))
+list_author_bibtool[${iauthor}]="Etourneau, Johan"
+list_author_title[${iauthor}]="Johan Etourneau"
+list_author_file[${iauthor}]="Etourneau_johan"
+#
 export list_author_file
 export list_author_title