Quatri�eme partie

Conclusion g�en�erale et bibliographie

Conclusion g�en�erale

Etant l'�emanation de la Sagesse desdites, les proverbes, on peuts'attendre qu'ils nous donnent la cl�e du monde, et on n'est pas�etonn�e. On l'a. C'est inutile car le monde n'est pas ferm�e, etsatisfaisant car la cl�e est un bel objet d�ecoratif.

Boris Vian

Dans le chapitre 3, nous avons analys�e les traces des points chauds actuels de laplaque Paci�que. Seuls quatre points chauds semblent satisfaire aux crit�eres associ�esaux mod�eles classiques (alimentation par un panache mantellique profond qui induit unelongue dur�ee de vie et un d�ebut d'activit�e marqu�ee par des �epanchements basaltiquesvolumineux) : Hawai'i, Louisville, Paques et, avec des r�eserves, les Marquises. En revanche,tous les points chauds du Paci�que sud, Samoa, Rarotonga, Rurutu, Soci�et�e, Australes-Macdonald, Pitcairn et Fondation sont des points chauds r�ecents, dont l'arriv�ee en surfacene correspond pas �a la formation de plateaux oc�eaniques. Leur lien avec un panachemantellique profond semble etre incompatible avec leur manifestation en surface. Cettepartie de l'�etude a mis en �evidence la divergence des points chauds polyn�esiens avec lesmod�eles classiques de type Hawai'i.

Dans le chapitre 4, nous avons montr�e que les caract�eristiques gravim�etriques des �lesdes archipels des Marquises, des Tuamotu, des Gambier, de la Soci�et�e et des Australes sontsimilaires �a celles de l'ensemble des volcans basaltiques. L'interpr�etation des anomaliesgravim�etriques r�esiduelles nous permet de d�e�nir la forme et l'emplacement des ancienneschambres magmatiques. La comparaison des r�esultats, obtenus sur 20 �les, nous a conduit�a proposer une relation lin�eaire entre le volume de l'�edi�ce volcanique et celui de lachambre magmatique fossile super�cielle. Cette relation s'applique �egalement au Pitondes Neiges, �a la R�eunion, mais pas au Kilauea, �a Hawai'i, probablement parce que lachambre magmatique de ce dernier ne s'est pas encore solidi��ee.

La campagne ZEPOLYF1 a mis en �evidence la pr�esence d'un vaste glissement sous-marin sur le anc sud de Tahiti. Le chapitre 5 a pr�esent�e l'analyse de ce glissement quenous a�ectons au type avalanche de d�ebris. De multiples �etudes sur la ride hawaiienne ontconclu que les ph�enom�enes de glissement dans les �les oc�eaniques font partie int�egrante du

192 Conclusion g�en�erale

processus de construction des �edi�ces basaltiques. Nous avons caract�eris�e le glissement deTahiti grace aux donn�ees d'imagerie acoustique, de bathym�etrie et de sismique r�e exion :la surface sous-marine sur laquelle s'�etalent les d�epots gliss�es est de 2945 km2, le volumedes d�ebris d'avalanche est estim�e �a 1154 km3. La zone de d�epart du glissement est le anca�erien sud de Tahiti Nui. Le comblement �a partir de 650 000 ans de cette zone par descoul�ees permet de situer la date du glissement entre 800 et 650 000 ans.

La troisi�eme partie de cette th�ese a �et�e consacr�ee �a l'�etude des provinces sous-marinesdes Tarava et des doubles rides Va'a Tau Piti. Ces provinces volcaniques ont �et�e compl�ete-ment cartographi�ees lors de la campagne ZEPOLYF1 (1996) sur le N/O L'Atalante et�echantillonn�ees lors de la campagne POLYDRAG (Bonneville et al., 1998). Deux agesradiom�etriques obtenus sur les �echantillons (35.9 et 43.6 Ma) viennent contraindre nosinterpr�etations.

La cha�ne sous-marine des monts Tarava est �etudi�ee dans le chapitre 6. L'analysemorphostructurale nous permet de la classer parmi les cha�nes volcaniques lin�eaires g�en�e-r�ees par un point chaud. Les monts Tarava sont caract�eris�es par 6 guyots dont la partiea�erienne disparue avait les caract�eristiques des �edi�ces des Australes : de petites �lesentour�ees de nombreux monts sous-marins. Comme les autres points chauds polyn�esiens,l'arriv�ee en surface du point chaud susceptible d'avoir cr�e�e les Tarava ne produit pasd'�epanchement basaltique volumineux. La �n de son activit�e pourrait se situer au niveaudes monts Taukina, juste au nord de l'alignement des Australes. Ce point chaud n'est plusactif actuellement. Sa trajectoire est fortement perturb�ee �a 43 Ma par un d�ecalage de 150km de son expression en surface. Nous associons ce d�ecalage �a l'in uence d'une directionde faiblesse majeure dans la lithosph�ere, que le syst�eme de conduits d'alimentation dupoint chaud n'arrive toutefois plus �a suivre au-del�a de 300 km de son point th�eoriquede sortie. Aux latitudes tropicales de la zone d'�etude, la subsidence normale du plancheroc�eanique est compens�ee par la croissance des constructions coralliennes. Dans le cas desTarava, cette croissance s'est interrompue entre 5 et 3 Ma. Nous expliquons la profondeuractuelle des guyots des Tarava par une subsidence du plancher oc�eanique due �a la exurede la lithosph�ere sous le poids des volcans de la Soci�et�e depuis 4 Ma. En revanche, sansune connaissance plus pr�ecise de la date de mort du corail, nous ne pouvons pas a�rmeravec certitude que cette exure soit �a l'origine de l'arret de la croissance corallienne.

Les doubles rides Va'a Tau Piti ont fait l'objet du chapitre 7. Le calcul des carat�eris-tiques �elastiques de la lithosph�ere sous-jacente montre que ces rides sont contemporainesde la formation de la lithosph�ere, ce qui �xe leur age entre 71 et 65 Ma. Dans le d�etail,l'interpr�etation des donn�ees magn�etiques montre que leur formation est li�ee �a un processusde segmentation du second ordre de l'ancienne dorsale Paci�que-Farallon. Les rides Va'aTau Piti se sont form�ees sur un segment de dorsale dont la vitesse d'accr�etion �etait plusrapide que celle du segment nord. La limite entre ces deux segments est identi�able parle d�ecalage des anomalies magn�etiques enregistr�ees par la croute. Des rides similairesse trouvant �a l'ouest de Tahiti et au nord des Tarava se sont form�ees suivant le memeprocessus lorsque le segment nord �etait plus rapide. L'ensemble de ces rides s'est doncform�e entre 84 et 65 Ma. Or, la segmentation provient des variations du bilan magmatique

Conclusion g�en�erale 193

sous la dorsale qui peuvent etre reli�ees aux r�eorganisations de fronti�eres de plaque (Macdo-nald et al., 1988). Nous pensons qu'il est possible que la r�eorganisation majeure desfronti�eres d'accr�etion Paci�que-Aluk-Bellingshausen entre 84 et 65 Ma, quelques 1300 kmplus au sud �a l'�epoque de la formation des rides, puisse en etre la cause.

156W 154W 152W 150W 148W

20S

18S

16S

156W 154W 152W 150W 148W

20S

18S

16S

156W 154W 152W 150W 148W

20S

18S

16S

*Tahiti

Iles de la Société

(4.2 Ma à l'actuel)

Tuamotu

Atollsisolés

Monts Tarava

(~47 à 31 Ma)Rides Va'a Tau Piti

(~71 à 65 M)

Ride nord et sud Tahiti(~74 Ma)

Rides nord Tarava(~84 à 74 Ma)

43.635.9

Fig. 7.12 { R�epartition des �episodes volcaniques dans la zone d'�etude : sous les nomsassoci�es �a chaque �episode se trouve l'age des formations volcaniques. Seuls les ages dela Soci�et�e sont connus avec certitude. L'age de l'ensemble de la cha�ne des Tarava estcontraint par 2 datations radiom�etriques report�ees en italique. L'age des rides a �et�e d�eduitdes caract�eriques �elastiques de la lithosph�ere. L'origine et l'age des trois atolls du nord-ouest sont inconnus.

Dans une r�egion o�u seule la cha�ne des volcans de la Soci�et�e �etait connue, notre travaila montr�e le caract�ere discontinu et de courte dur�ee du volcanisme depuis 84 Ma (Figure7.12). Ce comportement, qui s'�ecarte du mod�ele classique de point chaud, semble doncbien etre la r�egle plus que l'exception dans le Paci�que central sud, depuis la cr�eation dela lithosph�ere �a la dorsale jusqu'�a l'actuel.

Ce travail a �et�e r�ealis�e �a la suite d'acquisition de donn�ees lors de 3 campagnes �a lamer et une mission de reconnaissance g�eologique sur l'�le de Tahiti. Il a donn�e lieu �a unarticle accept�e, un article soumis et �a 3 pr�esentations dans des congr�es.

194

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