Quatri eme partie Conclusion - Institut de Physique du Globe de Paris

Quatrieme partie
Conclusion generale et bibliographie
Conclusion generale
Etant l'emanation de la Sagesse desdites, les proverbes, on peut
s'attendre qu'ils nous donnent la cle du monde, et on n'est pas
etonne. On l'a. C'est inutile car le monde n'est pas ferme, et
satisfaisant car la cle est un bel objet decoratif.
Boris Vian
Dans le chapitre 3, nous avons analyse les traces des points chauds actuels de la
plaque Pacique. Seuls quatre points chauds semblent satisfaire aux criteres associes
aux modeles classiques (alimentation par un panache mantellique profond qui induit une
longue duree de vie et un debut d'activite marquee par des epanchements basaltiques
volumineux) : Hawai'i, Louisville, P^aques et, avec des reserves, les Marquises. En revanche,
tous les points chauds du Pacique sud, Samoa, Rarotonga, Rurutu, Societe, AustralesMacdonald, Pitcairn et Fondation sont des points chauds recents, dont l'arrivee en surface
ne correspond pas a la formation de plateaux oceaniques. Leur lien avec un panache
mantellique profond semble ^etre incompatible avec leur manifestation en surface. Cette
partie de l'etude a mis en evidence la divergence des points chauds polynesiens avec les
modeles classiques de type Hawai'i.
Dans le chapitre 4, nous avons montre que les caracteristiques gravimetriques des ^les
des archipels des Marquises, des Tuamotu, des Gambier, de la Societe et des Australes sont
similaires a celles de l'ensemble des volcans basaltiques. L'interpretation des anomalies
gravimetriques residuelles nous permet de denir la forme et l'emplacement des anciennes
chambres magmatiques. La comparaison des resultats, obtenus sur 20 ^les, nous a conduit
a proposer une relation lineaire entre le volume de l'edice volcanique et celui de la
chambre magmatique fossile supercielle. Cette relation s'applique egalement au Piton
des Neiges, a la Reunion, mais pas au Kilauea, a Hawai'i, probablement parce que la
chambre magmatique de ce dernier ne s'est pas encore solidiee.
La campagne ZEPOLYF1 a mis en evidence la presence d'un vaste glissement sousmarin sur le anc sud de Tahiti. Le chapitre 5 a presente l'analyse de ce glissement que
nous aectons au type avalanche de debris. De multiples etudes sur la ride hawaiienne ont
conclu que les phenomenes de glissement dans les ^les oceaniques font partie integrante du
192
Conclusion generale
processus de construction des edices basaltiques. Nous avons caracterise le glissement de
Tahiti gr^ace aux donnees d'imagerie acoustique, de bathymetrie et de sismique reexion :
la surface sous-marine sur laquelle s'etalent les dep^ots glisses est de 2945 km2, le volume
des debris d'avalanche est estime a 1154 km3. La zone de depart du glissement est le anc
aerien sud de Tahiti Nui. Le comblement a partir de 650 000 ans de cette zone par des
coulees permet de situer la date du glissement entre 800 et 650 000 ans.
La troisieme partie de cette these a ete consacree a l'etude des provinces sous-marines
des Tarava et des doubles rides Va'a Tau Piti. Ces provinces volcaniques ont ete completement cartographiees lors de la campagne ZEPOLYF1 (1996) sur le N/O L'Atalante et
echantillonnees lors de la campagne POLYDRAG (Bonneville et al., 1998). Deux a^ges
radiometriques obtenus sur les echantillons (35.9 et 43.6 Ma) viennent contraindre nos
interpretations.
La cha^ne sous-marine des monts Tarava est etudiee dans le chapitre 6. L'analyse
morphostructurale nous permet de la classer parmi les cha^nes volcaniques lineaires generees par un point chaud. Les monts Tarava sont caracterises par 6 guyots dont la partie
aerienne disparue avait les caracteristiques des edices des Australes : de petites ^les
entourees de nombreux monts sous-marins. Comme les autres points chauds polynesiens,
l'arrivee en surface du point chaud susceptible d'avoir cree les Tarava ne produit pas
d'epanchement basaltique volumineux. La n de son activite pourrait se situer au niveau
des monts Taukina, juste au nord de l'alignement des Australes. Ce point chaud n'est plus
actif actuellement. Sa trajectoire est fortement perturbee a 43 Ma par un decalage de 150
km de son expression en surface. Nous associons ce decalage a l'inuence d'une direction
de faiblesse majeure dans la lithosphere, que le systeme de conduits d'alimentation du
point chaud n'arrive toutefois plus a suivre au-dela de 300 km de son point theorique
de sortie. Aux latitudes tropicales de la zone d'etude, la subsidence normale du plancher
oceanique est compensee par la croissance des constructions coralliennes. Dans le cas des
Tarava, cette croissance s'est interrompue entre 5 et 3 Ma. Nous expliquons la profondeur
actuelle des guyots des Tarava par une subsidence du plancher oceanique due a la exure
de la lithosphere sous le poids des volcans de la Societe depuis 4 Ma. En revanche, sans
une connaissance plus precise de la date de mort du corail, nous ne pouvons pas armer
avec certitude que cette exure soit a l'origine de l'arr^et de la croissance corallienne.
Les doubles rides Va'a Tau Piti ont fait l'objet du chapitre 7. Le calcul des carateristiques elastiques de la lithosphere sous-jacente montre que ces rides sont contemporaines
de la formation de la lithosphere, ce qui xe leur a^ge entre 71 et 65 Ma. Dans le detail,
l'interpretation des donnees magnetiques montre que leur formation est liee a un processus
de segmentation du second ordre de l'ancienne dorsale Pacique-Farallon. Les rides Va'a
Tau Piti se sont formees sur un segment de dorsale dont la vitesse d'accretion etait plus
rapide que celle du segment nord. La limite entre ces deux segments est identiable par
le decalage des anomalies magnetiques enregistrees par la cro^ute. Des rides similaires
se trouvant a l'ouest de Tahiti et au nord des Tarava se sont formees suivant le m^eme
processus lorsque le segment nord etait plus rapide. L'ensemble de ces rides s'est donc
forme entre 84 et 65 Ma. Or, la segmentation provient des variations du bilan magmatique
Conclusion generale
193
sous la dorsale qui peuvent ^etre reliees aux reorganisations de frontieres de plaque (Macdonald et al., 1988). Nous pensons qu'il est possible que la reorganisation majeure des
frontieres d'accretion Pacique-Aluk-Bellingshausen entre 84 et 65 Ma, quelques 1300 km
plus au sud a l'epoque de la formation des rides, puisse en ^etre la cause.
Tuamotu
Iles
(4.2 de la
Ma Soci
à l'a été
ctu
el)
Atolls
isolés
Ride nord et
sud Tahiti
(~74 Ma)
Tahiti
*
Mo
Rides nord Tarava
(~4 nts T
(~84 à 74 Ma)
7 à ara
v
a
3
43.6
1M
a)
35.9
Rides Va'a Tau Piti
(~71 à 65 M)
156W
154W
152W
16S
150W
18S
20S
148W
7.12 { Repartition des episodes volcaniques dans la zone d'etude : sous les noms
associes a chaque episode se trouve l'^age des formations volcaniques. Seuls les ^ages de
la Societe sont connus avec certitude. L'^age de l'ensemble de la cha^ne des Tarava est
contraint par 2 datations radiometriques reportees en italique. L'^age des rides a ete deduit
des caracteriques elastiques de la lithosphere. L'origine et l'^age des trois atolls du nordouest sont inconnus.
Fig.
Dans une region ou seule la cha^ne des volcans de la Societe etait connue, notre travail
a montre le caractere discontinu et de courte duree du volcanisme depuis 84 Ma (Figure
7.12). Ce comportement, qui s'ecarte du modele classique de point chaud, semble donc
bien ^etre la regle plus que l'exception dans le Pacique central sud, depuis la creation de
la lithosphere a la dorsale jusqu'a l'actuel.
Ce travail a ete realise a la suite d'acquisition de donnees lors de 3 campagnes a la
mer et une mission de reconnaissance geologique sur l'^le de Tahiti. Il a donne lieu a un
article accepte, un article soumis et a 3 presentations dans des congres.
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