AustralieFrV1, PascalFrancis, Curation, bibRecord, 003C01

The Role of Oceanic Heat Transport and Wind Stress Forcing in Abrupt Millennial-Scale Climate Transitions

Identifieur interne : 003C01 ( PascalFrancis/Curation ); précédent : 003C00; suivant : 003C02

The Role of Oceanic Heat Transport and Wind Stress Forcing in Abrupt Millennial-Scale Climate Transitions

Auteurs : Olivier Arzel [Australie] ; Alain Colin De Verdiere [France] ; Matthew H. England [Australie]

Source :

Journal of climate [ 0894-8755 ] ; 2010.

RBID : Pascal:10-0424548

Descripteurs français

Pascal (Inist)
- Action vent, Paléoclimat, Période glaciaire, Evénement Dansgaard-Oeschger, Circulation thermohaline, Glace marine, Instabilité, Stabilité, Holocène, Oscillation libre, Climat froid, Variation brusque, Eau douce, Climat chaud, Stratification, Refroidissement, Modèle climat, Eau fond, Masse eau, Variation interdécennale, Océan Atlantique Nord, Transport, Transfert chaleur, Variation climatique, Paléo-océanographie, Climatologie, Forçage, Eau surface, Contrôle climatique, Température surface, Zonation, Modèle couplé.
Wicri :
- topic : Eau douce, Climatologie.

English descriptors

KwdEn :
- Climate models, Climatology, Cold climate, Coupled model, Dansgaard-Oeschger events, Forcing, Free oscillation, Holocene, Hot climate, Interdecadal variation, North Atlantic, Sudden variation, Water mass, Wind effect, bottom water, climate variations, climatic controls, cooling, fresh water, glacial periods, heat transfer, instability, paleo-oceanography, paleoclimate, sea ice, stability, stratification, surface temperature, surface water, thermohaline circulation, transport, zoning.

Abstract

The last glacial period was punctuated by rapid climate shifts, known as Dansgaard-Oeschger events, with strong imprint in the North Atlantic sector suggesting that they were linked with the Atlantic meridional overturning circulation. Here an idealized single-hemisphere three-dimensional ocean-atmosphere-sea ice coupled model is used to explore the possible origin of the instability driving these abrupt events and to provide a plausible explanation for the relative stability of the Holocene. Focusing on the physics of noise-free millennial oscillations under steady external (solar) forcing, it was shown that cold climates become unstable, that is, exhibit abrupt millennial-scale transitions, for significantly lower freshwater fluxes than warm climates, in agreement with previous studies making use of zonally averaged coupled models. This fundamental difference is a direct consequence of the weaker stratification of the glacial ocean, mainly caused by upper-ocean cooling. Using a two-hemisphere configuration of a coupled climate model of intermediate complexity, it is shown that this result is robust to the added presence of a bottom water mass of southern origin. The analysis reveals that under particular conditions, a pronounced interdecadal variability develops during warm interstadials. While the nature of the instability driving the millennial oscillations is identical to that found in ocean models under mixed boundary conditions, these interstadial-interdecadal oscillations share the same characteristics as those previously found in ocean models forced by fixed surface fluxes. The wind stress forcing is shown to profoundly affect both the properties and bifurcation structure of thermohaline millennial oscillations across a wide range of variation of freshwater forcing. In particular, it is shown that the wind stress forcing favors the maintenance of thermally direct meridional overturning circulations during the cold stadial phases of Dansgaard-Oeschger cycles.

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C01	`01`		`ENG`	@0 The last glacial period was punctuated by rapid climate shifts, known as Dansgaard-Oeschger events, with strong imprint in the North Atlantic sector suggesting that they were linked with the Atlantic meridional overturning circulation. Here an idealized single-hemisphere three-dimensional ocean-atmosphere-sea ice coupled model is used to explore the possible origin of the instability driving these abrupt events and to provide a plausible explanation for the relative stability of the Holocene. Focusing on the physics of noise-free millennial oscillations under steady external (solar) forcing, it was shown that cold climates become unstable, that is, exhibit abrupt millennial-scale transitions, for significantly lower freshwater fluxes than warm climates, in agreement with previous studies making use of zonally averaged coupled models. This fundamental difference is a direct consequence of the weaker stratification of the glacial ocean, mainly caused by upper-ocean cooling. Using a two-hemisphere configuration of a coupled climate model of intermediate complexity, it is shown that this result is robust to the added presence of a bottom water mass of southern origin. The analysis reveals that under particular conditions, a pronounced interdecadal variability develops during warm interstadials. While the nature of the instability driving the millennial oscillations is identical to that found in ocean models under mixed boundary conditions, these interstadial-interdecadal oscillations share the same characteristics as those previously found in ocean models forced by fixed surface fluxes. The wind stress forcing is shown to profoundly affect both the properties and bifurcation structure of thermohaline millennial oscillations across a wide range of variation of freshwater forcing. In particular, it is shown that the wind stress forcing favors the maintenance of thermally direct meridional overturning circulations during the cold stadial phases of Dansgaard-Oeschger cycles.
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Le document en format XML

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<sourceDesc><biblStruct><analytic><title xml:lang="en" level="a">The Role of Oceanic Heat Transport and Wind Stress Forcing in Abrupt Millennial-Scale Climate Transitions</title>
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<profileDesc><textClass><keywords scheme="KwdEn" xml:lang="en"><term>Climate models</term>
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<term>Dansgaard-Oeschger events</term>
<term>Forcing</term>
<term>Free oscillation</term>
<term>Holocene</term>
<term>Hot climate</term>
<term>Interdecadal variation</term>
<term>North Atlantic</term>
<term>Sudden variation</term>
<term>Water mass</term>
<term>Wind effect</term>
<term>bottom water</term>
<term>climate variations</term>
<term>climatic controls</term>
<term>cooling</term>
<term>fresh water</term>
<term>glacial periods</term>
<term>heat transfer</term>
<term>instability</term>
<term>paleo-oceanography</term>
<term>paleoclimate</term>
<term>sea ice</term>
<term>stability</term>
<term>stratification</term>
<term>surface temperature</term>
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<term>Paléoclimat</term>
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<term>Evénement Dansgaard-Oeschger</term>
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<term>Glace marine</term>
<term>Instabilité</term>
<term>Stabilité</term>
<term>Holocène</term>
<term>Oscillation libre</term>
<term>Climat froid</term>
<term>Variation brusque</term>
<term>Eau douce</term>
<term>Climat chaud</term>
<term>Stratification</term>
<term>Refroidissement</term>
<term>Modèle climat</term>
<term>Eau fond</term>
<term>Masse eau</term>
<term>Variation interdécennale</term>
<term>Océan Atlantique Nord</term>
<term>Transport</term>
<term>Transfert chaleur</term>
<term>Variation climatique</term>
<term>Paléo-océanographie</term>
<term>Climatologie</term>
<term>Forçage</term>
<term>Eau surface</term>
<term>Contrôle climatique</term>
<term>Température surface</term>
<term>Zonation</term>
<term>Modèle couplé</term>
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<keywords scheme="Wicri" type="topic" xml:lang="fr"><term>Eau douce</term>
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<front><div type="abstract" xml:lang="en">The last glacial period was punctuated by rapid climate shifts, known as Dansgaard-Oeschger events, with strong imprint in the North Atlantic sector suggesting that they were linked with the Atlantic meridional overturning circulation. Here an idealized single-hemisphere three-dimensional ocean-atmosphere-sea ice coupled model is used to explore the possible origin of the instability driving these abrupt events and to provide a plausible explanation for the relative stability of the Holocene. Focusing on the physics of noise-free millennial oscillations under steady external (solar) forcing, it was shown that cold climates become unstable, that is, exhibit abrupt millennial-scale transitions, for significantly lower freshwater fluxes than warm climates, in agreement with previous studies making use of zonally averaged coupled models. This fundamental difference is a direct consequence of the weaker stratification of the glacial ocean, mainly caused by upper-ocean cooling. Using a two-hemisphere configuration of a coupled climate model of intermediate complexity, it is shown that this result is robust to the added presence of a bottom water mass of southern origin. The analysis reveals that under particular conditions, a pronounced interdecadal variability develops during warm interstadials. While the nature of the instability driving the millennial oscillations is identical to that found in ocean models under mixed boundary conditions, these interstadial-interdecadal oscillations share the same characteristics as those previously found in ocean models forced by fixed surface fluxes. The wind stress forcing is shown to profoundly affect both the properties and bifurcation structure of thermohaline millennial oscillations across a wide range of variation of freshwater forcing. In particular, it is shown that the wind stress forcing favors the maintenance of thermally direct meridional overturning circulations during the cold stadial phases of Dansgaard-Oeschger cycles.</div>
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<fA11 i1="02" i2="1"><s1>DE VERDIERE (Alain Colin)</s1>
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<fA11 i1="03" i2="1"><s1>ENGLAND (Matthew H.)</s1>
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<fA14 i1="01"><s1>Climate Change Research Centre, The University of New South Wales</s1>
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<fA14 i1="02"><s1>Laboratoire de Physique des Océans, Université de Bretagne Occidentale</s1>
<s2>Brest</s2>
<s3>FRA</s3>
<sZ>2 aut.</sZ>
</fA14>
<fA20><s1>2233-2256</s1>
</fA20>
<fA21><s1>2010</s1>
</fA21>
<fA23 i1="01"><s0>ENG</s0>
</fA23>
<fA43 i1="01"><s1>INIST</s1>
<s2>9644B</s2>
<s5>354000170430930010</s5>
</fA43>
<fA44><s0>0000</s0>
<s1>© 2010 INIST-CNRS. All rights reserved.</s1>
</fA44>
<fA45><s0>1 p.3/4</s0>
</fA45>
<fA47 i1="01" i2="1"><s0>10-0424548</s0>
</fA47>
<fA60><s1>P</s1>
</fA60>
<fA61><s0>A</s0>
</fA61>
<fA64 i1="01" i2="1"><s0>Journal of climate</s0>
</fA64>
<fA66 i1="01"><s0>USA</s0>
</fA66>
<fC01 i1="01" l="ENG"><s0>The last glacial period was punctuated by rapid climate shifts, known as Dansgaard-Oeschger events, with strong imprint in the North Atlantic sector suggesting that they were linked with the Atlantic meridional overturning circulation. Here an idealized single-hemisphere three-dimensional ocean-atmosphere-sea ice coupled model is used to explore the possible origin of the instability driving these abrupt events and to provide a plausible explanation for the relative stability of the Holocene. Focusing on the physics of noise-free millennial oscillations under steady external (solar) forcing, it was shown that cold climates become unstable, that is, exhibit abrupt millennial-scale transitions, for significantly lower freshwater fluxes than warm climates, in agreement with previous studies making use of zonally averaged coupled models. This fundamental difference is a direct consequence of the weaker stratification of the glacial ocean, mainly caused by upper-ocean cooling. Using a two-hemisphere configuration of a coupled climate model of intermediate complexity, it is shown that this result is robust to the added presence of a bottom water mass of southern origin. The analysis reveals that under particular conditions, a pronounced interdecadal variability develops during warm interstadials. While the nature of the instability driving the millennial oscillations is identical to that found in ocean models under mixed boundary conditions, these interstadial-interdecadal oscillations share the same characteristics as those previously found in ocean models forced by fixed surface fluxes. The wind stress forcing is shown to profoundly affect both the properties and bifurcation structure of thermohaline millennial oscillations across a wide range of variation of freshwater forcing. In particular, it is shown that the wind stress forcing favors the maintenance of thermally direct meridional overturning circulations during the cold stadial phases of Dansgaard-Oeschger cycles.</s0>
</fC01>
<fC02 i1="01" i2="2"><s0>001E02D</s0>
</fC02>
<fC02 i1="02" i2="2"><s0>001E01H</s0>
</fC02>
<fC02 i1="03" i2="2"><s0>001E01P02</s0>
</fC02>
<fC02 i1="04" i2="2"><s0>223B</s0>
</fC02>
<fC02 i1="05" i2="2"><s0>226C02</s0>
</fC02>
<fC03 i1="01" i2="X" l="FRE"><s0>Action vent</s0>
<s5>01</s5>
</fC03>
<fC03 i1="01" i2="X" l="ENG"><s0>Wind effect</s0>
<s5>01</s5>
</fC03>
<fC03 i1="01" i2="X" l="SPA"><s0>Acción viento</s0>
<s5>01</s5>
</fC03>
<fC03 i1="02" i2="2" l="FRE"><s0>Paléoclimat</s0>
<s5>02</s5>
</fC03>
<fC03 i1="02" i2="2" l="ENG"><s0>paleoclimate</s0>
<s5>02</s5>
</fC03>
<fC03 i1="02" i2="2" l="SPA"><s0>Paleoclima</s0>
<s5>02</s5>
</fC03>
<fC03 i1="03" i2="2" l="FRE"><s0>Période glaciaire</s0>
<s5>03</s5>
</fC03>
<fC03 i1="03" i2="2" l="ENG"><s0>glacial periods</s0>
<s5>03</s5>
</fC03>
<fC03 i1="03" i2="2" l="SPA"><s0>Período glaciario</s0>
<s5>03</s5>
</fC03>
<fC03 i1="04" i2="2" l="FRE"><s0>Evénement Dansgaard-Oeschger</s0>
<s2>NX</s2>
<s5>04</s5>
</fC03>
<fC03 i1="04" i2="2" l="ENG"><s0>Dansgaard-Oeschger events</s0>
<s2>NX</s2>
<s5>04</s5>
</fC03>
<fC03 i1="05" i2="2" l="FRE"><s0>Circulation thermohaline</s0>
<s5>05</s5>
</fC03>
<fC03 i1="05" i2="2" l="ENG"><s0>thermohaline circulation</s0>
<s5>05</s5>
</fC03>
<fC03 i1="05" i2="2" l="SPA"><s0>Circulación termohalina</s0>
<s5>05</s5>
</fC03>
<fC03 i1="06" i2="2" l="FRE"><s0>Glace marine</s0>
<s5>06</s5>
</fC03>
<fC03 i1="06" i2="2" l="ENG"><s0>sea ice</s0>
<s5>06</s5>
</fC03>
<fC03 i1="06" i2="2" l="SPA"><s0>Hielo marino</s0>
<s5>06</s5>
</fC03>
<fC03 i1="07" i2="2" l="FRE"><s0>Instabilité</s0>
<s5>07</s5>
</fC03>
<fC03 i1="07" i2="2" l="ENG"><s0>instability</s0>
<s5>07</s5>
</fC03>
<fC03 i1="08" i2="2" l="FRE"><s0>Stabilité</s0>
<s5>08</s5>
</fC03>
<fC03 i1="08" i2="2" l="ENG"><s0>stability</s0>
<s5>08</s5>
</fC03>
<fC03 i1="08" i2="2" l="SPA"><s0>Estabilidad</s0>
<s5>08</s5>
</fC03>
<fC03 i1="09" i2="2" l="FRE"><s0>Holocène</s0>
<s2>NX</s2>
<s5>09</s5>
</fC03>
<fC03 i1="09" i2="2" l="ENG"><s0>Holocene</s0>
<s2>NX</s2>
<s5>09</s5>
</fC03>
<fC03 i1="09" i2="2" l="SPA"><s0>Holoceno</s0>
<s2>NX</s2>
<s5>09</s5>
</fC03>
<fC03 i1="10" i2="X" l="FRE"><s0>Oscillation libre</s0>
<s5>10</s5>
</fC03>
<fC03 i1="10" i2="X" l="ENG"><s0>Free oscillation</s0>
<s5>10</s5>
</fC03>
<fC03 i1="10" i2="X" l="SPA"><s0>Oscilación libre</s0>
<s5>10</s5>
</fC03>
<fC03 i1="11" i2="X" l="FRE"><s0>Climat froid</s0>
<s5>11</s5>
</fC03>
<fC03 i1="11" i2="X" l="ENG"><s0>Cold climate</s0>
<s5>11</s5>
</fC03>
<fC03 i1="11" i2="X" l="SPA"><s0>Clima frío</s0>
<s5>11</s5>
</fC03>
<fC03 i1="12" i2="X" l="FRE"><s0>Variation brusque</s0>
<s5>12</s5>
</fC03>
<fC03 i1="12" i2="X" l="ENG"><s0>Sudden variation</s0>
<s5>12</s5>
</fC03>
<fC03 i1="12" i2="X" l="SPA"><s0>Variación brusca</s0>
<s5>12</s5>
</fC03>
<fC03 i1="13" i2="2" l="FRE"><s0>Eau douce</s0>
<s5>13</s5>
</fC03>
<fC03 i1="13" i2="2" l="ENG"><s0>fresh water</s0>
<s5>13</s5>
</fC03>
<fC03 i1="13" i2="2" l="SPA"><s0>Agua dulce</s0>
<s5>13</s5>
</fC03>
<fC03 i1="14" i2="X" l="FRE"><s0>Climat chaud</s0>
<s5>14</s5>
</fC03>
<fC03 i1="14" i2="X" l="ENG"><s0>Hot climate</s0>
<s5>14</s5>
</fC03>
<fC03 i1="14" i2="X" l="SPA"><s0>Clima caliente</s0>
<s5>14</s5>
</fC03>
<fC03 i1="15" i2="2" l="FRE"><s0>Stratification</s0>
<s5>15</s5>
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<fC03 i1="15" i2="2" l="ENG"><s0>stratification</s0>
<s5>15</s5>
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<fC03 i1="15" i2="2" l="SPA"><s0>Estratificación</s0>
<s5>15</s5>
</fC03>
<fC03 i1="16" i2="2" l="FRE"><s0>Refroidissement</s0>
<s5>16</s5>
</fC03>
<fC03 i1="16" i2="2" l="ENG"><s0>cooling</s0>
<s5>16</s5>
</fC03>
<fC03 i1="16" i2="2" l="SPA"><s0>Enfriamiento</s0>
<s5>16</s5>
</fC03>
<fC03 i1="17" i2="3" l="FRE"><s0>Modèle climat</s0>
<s5>17</s5>
</fC03>
<fC03 i1="17" i2="3" l="ENG"><s0>Climate models</s0>
<s5>17</s5>
</fC03>
<fC03 i1="18" i2="2" l="FRE"><s0>Eau fond</s0>
<s5>18</s5>
</fC03>
<fC03 i1="18" i2="2" l="ENG"><s0>bottom water</s0>
<s5>18</s5>
</fC03>
<fC03 i1="18" i2="2" l="SPA"><s0>Agua fondo</s0>
<s5>18</s5>
</fC03>
<fC03 i1="19" i2="X" l="FRE"><s0>Masse eau</s0>
<s5>19</s5>
</fC03>
<fC03 i1="19" i2="X" l="ENG"><s0>Water mass</s0>
<s5>19</s5>
</fC03>
<fC03 i1="19" i2="X" l="SPA"><s0>Masa agua</s0>
<s5>19</s5>
</fC03>
<fC03 i1="20" i2="X" l="FRE"><s0>Variation interdécennale</s0>
<s5>20</s5>
</fC03>
<fC03 i1="20" i2="X" l="ENG"><s0>Interdecadal variation</s0>
<s5>20</s5>
</fC03>
<fC03 i1="20" i2="X" l="SPA"><s0>Variación interdecenal</s0>
<s5>20</s5>
</fC03>
<fC03 i1="21" i2="2" l="FRE"><s0>Océan Atlantique Nord</s0>
<s2>NG</s2>
<s5>21</s5>
</fC03>
<fC03 i1="21" i2="2" l="ENG"><s0>North Atlantic</s0>
<s2>NG</s2>
<s5>21</s5>
</fC03>
<fC03 i1="21" i2="2" l="SPA"><s0>Océano Atlántico Norte</s0>
<s2>NG</s2>
<s5>21</s5>
</fC03>
<fC03 i1="22" i2="2" l="FRE"><s0>Transport</s0>
<s5>22</s5>
</fC03>
<fC03 i1="22" i2="2" l="ENG"><s0>transport</s0>
<s5>22</s5>
</fC03>
<fC03 i1="22" i2="2" l="SPA"><s0>Transporte</s0>
<s5>22</s5>
</fC03>
<fC03 i1="23" i2="2" l="FRE"><s0>Transfert chaleur</s0>
<s5>23</s5>
</fC03>
<fC03 i1="23" i2="2" l="ENG"><s0>heat transfer</s0>
<s5>23</s5>
</fC03>
<fC03 i1="23" i2="2" l="SPA"><s0>Transferencia térmica</s0>
<s5>23</s5>
</fC03>
<fC03 i1="24" i2="2" l="FRE"><s0>Variation climatique</s0>
<s5>24</s5>
</fC03>
<fC03 i1="24" i2="2" l="ENG"><s0>climate variations</s0>
<s5>24</s5>
</fC03>
<fC03 i1="25" i2="2" l="FRE"><s0>Paléo-océanographie</s0>
<s5>25</s5>
</fC03>
<fC03 i1="25" i2="2" l="ENG"><s0>paleo-oceanography</s0>
<s5>25</s5>
</fC03>
<fC03 i1="26" i2="X" l="FRE"><s0>Climatologie</s0>
<s5>26</s5>
</fC03>
<fC03 i1="26" i2="X" l="ENG"><s0>Climatology</s0>
<s5>26</s5>
</fC03>
<fC03 i1="26" i2="X" l="SPA"><s0>Climatología</s0>
<s5>26</s5>
</fC03>
<fC03 i1="27" i2="X" l="FRE"><s0>Forçage</s0>
<s5>27</s5>
</fC03>
<fC03 i1="27" i2="X" l="ENG"><s0>Forcing</s0>
<s5>27</s5>
</fC03>
<fC03 i1="27" i2="X" l="SPA"><s0>Forzamiento</s0>
<s5>27</s5>
</fC03>
<fC03 i1="28" i2="2" l="FRE"><s0>Eau surface</s0>
<s5>61</s5>
</fC03>
<fC03 i1="28" i2="2" l="ENG"><s0>surface water</s0>
<s5>61</s5>
</fC03>
<fC03 i1="28" i2="2" l="SPA"><s0>Agua superficie</s0>
<s5>61</s5>
</fC03>
<fC03 i1="29" i2="2" l="FRE"><s0>Contrôle climatique</s0>
<s5>62</s5>
</fC03>
<fC03 i1="29" i2="2" l="ENG"><s0>climatic controls</s0>
<s5>62</s5>
</fC03>
<fC03 i1="30" i2="2" l="FRE"><s0>Température surface</s0>
<s5>64</s5>
</fC03>
<fC03 i1="30" i2="2" l="ENG"><s0>surface temperature</s0>
<s5>64</s5>
</fC03>
<fC03 i1="31" i2="2" l="FRE"><s0>Zonation</s0>
<s5>65</s5>
</fC03>
<fC03 i1="31" i2="2" l="ENG"><s0>zoning</s0>
<s5>65</s5>
</fC03>
<fC03 i1="31" i2="2" l="SPA"><s0>Zonalidad</s0>
<s5>65</s5>
</fC03>
<fC03 i1="32" i2="2" l="FRE"><s0>Modèle couplé</s0>
<s4>CD</s4>
<s5>96</s5>
</fC03>
<fC03 i1="32" i2="2" l="ENG"><s0>Coupled model</s0>
<s4>CD</s4>
<s5>96</s5>
</fC03>
<fC03 i1="32" i2="2" l="SPA"><s0>Modelo acoplado</s0>
<s4>CD</s4>
<s5>96</s5>
</fC03>
<fC07 i1="01" i2="2" l="FRE"><s0>Quaternaire sup</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="01" i2="2" l="ENG"><s0>upper Quaternary</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="01" i2="2" l="SPA"><s0>Cuaternario sup</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="02" i2="2" l="FRE"><s0>Quaternaire</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="02" i2="2" l="ENG"><s0>Quaternary</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="02" i2="2" l="SPA"><s0>Cuaternario</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="03" i2="2" l="FRE"><s0>Cénozoïque</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="03" i2="2" l="ENG"><s0>Cenozoic</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="03" i2="2" l="SPA"><s0>Cenozoico</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="04" i2="2" l="FRE"><s0>Phanérozoïque</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="04" i2="2" l="ENG"><s0>Phanerozoic</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="04" i2="2" l="SPA"><s0>Fanerozoico</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="05" i2="2" l="FRE"><s0>Océan Atlantique</s0>
<s2>564</s2>
</fC07>
<fC07 i1="05" i2="2" l="ENG"><s0>Atlantic Ocean</s0>
<s2>564</s2>
</fC07>
<fC07 i1="05" i2="2" l="SPA"><s0>Océano Atlántico</s0>
<s2>564</s2>
</fC07>
<fN21><s1>277</s1>
</fN21>
<fN44 i1="01"><s1>PSI</s1>
</fN44>
<fN82><s1>PSI</s1>
</fN82>
</pA>
</standard>
</inist>
</record>

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The Role of Oceanic Heat Transport and Wind Stress Forcing in Abrupt Millennial-Scale Climate Transitions

The Role of Oceanic Heat Transport and Wind Stress Forcing in Abrupt Millennial-Scale Climate Transitions

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