Relevant bibliographies by topics / Morondava

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Academic literature on the topic 'Morondava'

Author: Grafiati
Published: 4 June 2021
Last updated: 5 February 2022

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Journal articles on the topic "Morondava"

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Delatte, H., B. Reynaud, J. M. Lett, M. Peterschmitt, M. Granier, J. Ravololonandrianina, and W. R. Goldbach. "First Molecular Identification of a Begomovirus Isolated from Tomato in Madagascar." Plant Disease 86, no. 12 (December 2002): 1404. http://dx.doi.org/10.1094/pdis.2002.86.12.1404c.

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In April 2001, reduced leaf size, leaf curling, yellowing symptoms, and reduced yield were observed in tomato plants in the southwestern (Toliary, Morondava, Miandrivazo) and northern (Antsiranana) regions of Madagascar. Symptoms were similar to those caused by Tomato yellow leaf curl virus (TYLCV, genus Begomovirus, family Geminiviridae). Large populations of Bemisia tabaci (Gennadius) were observed colonizing tomato, other crops, and weeds. Leaf samples were collected from tomato plants from 14 sites located in northern, central, and southern Madagascar. Two plant samples collected near Antsiranana, one sample near Morondava, and one sample near Toliary were positive in triple-antibody sandwich enzyme-linked immunosorbent assay using a begomovirus-specific antibody purchased from ADGEN (Nellies Gates, Auchincruive, Scotland, UK). A 500-bp product was amplified and cloned (2) from two leaf samples collected near Toliary and one near Morondava using a pair of degenerate primers that are expected to amplify a region of the A component of begomoviruses between the intergenic conserved nonanucleotide sequence and the first 200 nucleotides of the coat protein ORF. The sequences corresponding to the two Toliary samples (GenBank Accession Nos. AJ422123 and AJ422124) and the Morondava sample (GenBank No. AJ422125) showed the most significant alignments (NCBI, BLAST) with begomoviruses, Tobacco leaf curl virus from Zimbabwe (GenBank Accession No. AF 350330) and Tomato leaf curl virus from Tanzania (GenBank Accession No. U73498) with 76 to 77% nucleotide identity (Clustal method, MegAlign, DNASTAR, London) and South African cassava mosaic viruses (SACMV GenBank Accession Nos. AJ422132 and AF155806) and East African cassava mosaic viruses from Malawi (GenBank Accession Nos. AJ006459 and AJ006460) with 74 to 75.5% nucleotide identity. The low nucleotide identity suggests that the begomovirus isolated from tomato in Madagascar is a new species. Since the core region of the coat protein gene is a molecular marker for provisional classification of begomoviruses (1), this region was amplified for the Morondava isolate with degenerate primers. The 519nt core fragment obtained showed the most significant alignments with SACMV (GenBank Accession No. AF329227), Cassava geminivirus from Mozambique (GenBank Accession No. AF329240), and with TYLCV (GenBank Accession Nos. AB014346 and AF105975) with 81 to 82% nucleotide identity. According to the current taxonomic criteria (4), the begomovirus from Madagascar is a new one that is related to begomoviruses from the southern part of Africa and to TYLCV and is provisionally named Tomato yellow leaf curl Morondava virus (TYLCMV). Tomato yellow leaf curl disease was previously described in Madagascar by Reckhaus (3) who presumed that it was caused by TYLCV. Although symptoms in the tomato plant from which TYLCMV was isolated were similar to those induced by TYLCV, TYLCV was not detected in our samples. References: (1) J. K. Brown et al. Arch. Virol. 146:1581, 2001 (2) M. Peterschmitt et al. Plant Dis. 83:303, 1999. (3) P. Reckhaus, Maladies et ravageurs des cultures maraîchères: A l'exemple de Madagascar. GTZ, Weikersem, 1997. (4) M. H. V. van Regenmortel et al. Virus Taxonomy. Seventh Rep. Int. Comm. Taxon. Viruses. Academic Press, San Diego, 2000.
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Kennedy, William James, Ireneusz Walaszczyk, Andrew S. Gale, Krzysztof Dembicz, and Tomasz Praszkier. "Lower and Middle Cenomanian ammonites from the Morondava Basin, Madagascar." Acta Geologica Polonica 63, no. 4 (December 1, 2013): 625–55. http://dx.doi.org/10.2478/agp-2013-0027.

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ABSTRACT Kennedy, W.J., Walaszczyk, I., Gale, A.S., Dembicz, K. and Praszkier, T. 2013. Lower and Midle Cenomanian ammonites from the Morondava Basin, Madagascar. Acta Geologica Polonica, 63(4), 625-655. Warszawa. Lower and Middle Cenomanian ammonite assemblages have been collected on a bed-by-bed basis from localities at Vohipaly and Mahaboboka, Madagascar, as well as from outcrops around Berekata, all in the Morondava Basin, southwest Madagascar. These collections demonstrate the presence of the upper Lower Cenomanian Mantelliceras dixoni Zone and the lower Middle Cenomanian Cunningtoniceras inerme Zone of the north-western European standard sequence. These records indicate that the striking anomalies in the zonal assemblages of the classic divisions of the Madagascan Cenomanian are based on mixed assemblages, rather than a succession that differs radically from that elsewhere in the world. The dixoni Zone fauna is: Desmoceras cf. latidorsatum (Michelin, 1838), Pachydesmoceras kossmati Matsumoto, 1987, Forbesiceras sp., F. baylissiWright & Kennedy, 1984, F. largilliertianum (d’Orbigny, 1841), Mantelliceras cantianum Spath, 1926a, M. dixoni Spath, 1926b, M. mantelli (J. Sowerby, 1814), M. picteti Hyatt, 1903, M. saxbii (Sharpe, 1857), Sharpeiceras sp., S. falloti (Collignon, 1931), S. mocambiquense (Choffat, 1903), S. cf. florencae Spath, 1925, Acompsoceras renevieri (Sharpe, 1857), A. tenue Collignon, 1964, Calycoceras sp., Mrhiliceras lapparenti (Pervinquière, 1907), Mariella (Mariella) stolizcai (Collignon, 1964), Hypoturrilites taxyfabreae (Collignon, 1964), Turrilites scheuchzerianus Bosc, 1801, Sciponoceras cucullatum Collignon, 1964, and Sciponoceras antanimangaensis (Collignon, 1964). The presence of Calycoceras in a Lower Cenomanian association represents a precocious appearance of a genus typically Middle and Upper Cenomanian in occurrence, and matches records from Tunisia. The inerme Zone yields a more restricted assemblage: Pachydesmoceras kossmati, Forbesiceras baylissi, Acanthoceras sp. juv., Cunningtoniceras cunningtoni (Sharpe, 1855) and Hypoturrilites taxyfabreae.
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Bardintzeff, J. M., B. Bonin, and G. Rasamimanana. "The Cretaceous morondava volcanic province (West Madagascar): mineralogical, petrological and geochemical aspects." Journal of African Earth Sciences 32, no. 2 (February 2001): 299–316. http://dx.doi.org/10.1016/s0899-5362(01)90008-9.

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Sorg, Jean-Pierre. "Organisation de la recherche dans les zones sèches un cas concret dans l'ouest de Madagascar | Design of Forest Research in Dry Zones -a Case Study in the West of Madagascar." Schweizerische Zeitschrift fur Forstwesen 151, no. 3 (March 1, 2000): 84–86. http://dx.doi.org/10.3188/szf.2000.0084.

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An interesting research programme focusing on trees and forest,which has been continuing in the region of Morondava for more than 20 years, presently finds itself in an environment somewhat unfavourable for research and, therefore, is in an evaluative phase. While at the beginning the emphasis was strongly put on forestry, the programme developed more and more towards the interface mankind – forest, and through social-forestry activities progressively towards the population of the villages. Today, it is clear that research on participative management of forests and the scientific interest in natural eco-systems and their dynamics are complementary and have to be co-ordinated with regard to sustainability.
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Rindraharisaona, E. J., F. Tilmann, X. Yuan, J. Dreiling, J. Giese, K. Priestley, and G. Rümpker. "Velocity structure and radial anisotropy of the lithosphere in southern Madagascar from surface wave dispersion." Geophysical Journal International 224, no. 3 (November 17, 2020): 1930–44. http://dx.doi.org/10.1093/gji/ggaa550.

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SUMMARY We investigate the upper mantle seismic structure beneath southern Madagascar and infer the imprint of geodynamic events since Madagascar’s break-up from Africa and India and earlier rifting episodes. Rayleigh and Love wave phase velocities along a profile across southern Madagascar were determined by application of the two-station method to teleseismic earthquake data. For shorter periods (<20 s), these data were supplemented by previously published dispersion curves determined from ambient noise correlation. First, tomographic models of the phase velocities were determined. In a second step, 1-D models of SV and SH wave velocities were inverted based on the dispersion curves extracted from the tomographic models. As the lithospheric mantle is represented by high velocities we identify the lithosphere–asthenosphere boundary by the strongest negative velocity gradient. Finally, the radial anisotropy (RA) is derived from the difference between the SV and SH velocity models. An additional constraint on the lithospheric thickness is provided by the presence of a negative conversion seen in S receiver functions, which results in comparable estimates under most of Madagascar. We infer a lithospheric thickness of 110−150 km beneath southern Madagascar, significantly thinner than beneath the mobile belts in East Africa (150−200 km), where the crust is of comparable age and which were located close to Madagascar in Gondwanaland. The lithospheric thickness is correlated with the geological domains. The thinnest lithosphere (∼110 km) is found beneath the Morondava basin. The pre-breakup Karoo failed rifting, the rifting and breakup of Gondwanaland have likely thinned the lithosphere there. The thickness of the lithosphere in the Proterozoic terranes (Androyen and Anosyen domains) ranges from 125 to 140 km, which is still ∼30 km thinner than in the Mozambique belt in Tanzania. The lithosphere is the thickest beneath Ikalamavony domain (Proterozoic) and the west part of the Antananarivo domain (Archean) with a thickness of ∼150 km. Below the eastern part of Archean domain the lithosphere thickness reduces to ∼130 km. The lithosphere below the entire profile is characterized by positive RA. The strongest RA is observed in the uppermost mantle beneath the Morondava basin (maximum value of ∼9 per cent), which is understandable from the strong stretching that the basin was exposed to during the Karoo and subsequent rifting episode. Anisotropy is still significantly positive below the Proterozoic (maximum value of ∼5 per cent) and Archean (maximum value of ∼6 per cent) domains, which may result from lithospheric extension during the Mesozoic and/or thereafter. In the asthenosphere, a positive RA is observed beneath the eastern part Morondava sedimentary basin and the Proterozoic domain, indicating a horizontal asthenospheric flow pattern. Negative RA is found beneath the Archean in the east, suggesting a small-scale asthenospheric upwelling, consistent with previous studies. Alternatively, the relatively high shear wave velocity in the asthenosphere in this region indicate that the negative RA could be associated to the Réunion mantle plume, at least beneath the volcanic formation, along the eastern coast.
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Nichols, G. J., and M. C. Daly. "Sedimentation in an intracratonic extensional basin: the Karoo of the Central Morondava Basin, Madagascar." Geological Magazine 126, no. 4 (July 1989): 339–54. http://dx.doi.org/10.1017/s0016756800006543.

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AbstractThe late Carboniferous to Triassic Karoo Supergroup of Madagascar is a sequence of predominantly continental clastic sediments deposited during a long period of regional crustal extension. In the Morondava Basin of western Madagascar the lower two divisions of the Karoo sediments – the Sakoa and the Sakamena – are deposits of fluvial and lacustrine sedimentation systems supplied from the Precambrian metamorphic basement terrain to the east. East–west crustal extension produced a series of graben and half-graben structures after the Sakoa period which were reactivated after the Sakamena. The position and orientation of these half graben, which were marginal to a larger rift system to the west, were partly controlled by the steep NNE–SSW mylonitic fabric in the metamorphic basement. Palaeocurrents in the braided river deposits of the Sakoa and Lower Sakamena indicate flow to the southwest and west in both sequences. The rivers followed a regional palaeoslope to the southwest/west and were apparently not significantly influenced by the local structural trends which were oriented perpendicular to this slope. The absence of local structural control is attributed to extensive erosional events which followed each tectonic episode and preceded the onset of further sedimentation which took place on an essentially peneplained surface. The tectonic episodes brought about changes in base level which caused this part of the basin to fluctuate between erosion and deposition.
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Schandelmeier, H., F. Bremer, and H. G. Holl. "Kinematic evolution of the Morondava rift basin of SW Madagascar––from wrench tectonics to normal extension." Journal of African Earth Sciences 38, no. 4 (March 2004): 321–30. http://dx.doi.org/10.1016/j.jafrearsci.2003.11.002.

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Giese, Jörg, Diane Seward, and Guido Schreurs. "Low-temperature evolution of the Morondava rift basin shoulder in western Madagascar: An apatite fission track study." Tectonics 31, no. 2 (March 23, 2012): n/a. http://dx.doi.org/10.1029/2011tc002921.

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Geiger, Markus, and Günter Schweigert. "Toarcian–Kimmeridgian depositional cycles of the south-western Morondava Basin along the rifted continental margin of Madagascar." Facies 52, no. 1 (February 14, 2006): 85–112. http://dx.doi.org/10.1007/s10347-005-0039-8.

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Wescott, William A., and John N. Diggens. "Depositional history and stratigraphical evolution of the Sakoa Group (Lower Karoo Supergroup) in the southern Morondava Basin, Madagascar." Journal of African Earth Sciences 24, no. 4 (May 1997): 585–601. http://dx.doi.org/10.1016/s0899-5362(97)00082-1.

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Dissertations / Theses on the topic "Morondava"

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Bremer, Florian Heinrich. "Karoo rifting im Morondava Becken, Madagaskar: fazielle Entwicklung, Kinematik und Dynamik eines polyphasen Riftbeckens." [S.l.] : [s.n.], 2005. http://deposit.ddb.de/cgi-bin/dokserv?idn=975019910.

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Razafimbelo, Eugène. "Le Bassin de Morondava (Madagascar) synthèse géologique et structurale /." Grenoble 2 : ANRT, 1987. http://catalogue.bnf.fr/ark:/12148/cb376092243.

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Razafimbelo, Eugène. "Le bassin de morondava (madagascar) : synthese geologique et structurale." Université Louis Pasteur (Strasbourg) (1971-2008), 1987. http://www.theses.fr/1987STR13184.

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La synthese des donnees geologiques et structurales du bassin de morondava conduit a modifier la nomenclature stratigraphique des formations sedimentaires du type "karroo". Dans le bassin, le controle tectonique de la sedimentation est realise par un jeu complexe mais permanent de failles en faisceaux denses. La fracturation continentale a permis la mise en place de roches effusives basaltes et gabbros, puis roches granito-syenitiques. L'epaisseur et la nature des formations sedimentaires du bassin de morondava sont propices a la naissance de gisements d'hydrocarbures
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Delaunay, Antoine. "Les mouvements verticaux de Madagascar (90 - 0 Ma) : une analyse couplée des formes du relief et de l'enregistrement sédimentaire des marges ouest malgaches." Thesis, Rennes 1, 2018. http://www.theses.fr/2018REN1B006/document.

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Madagascar est un lambeau de croûte continentale archéenne à néoproterozoïque entouré de marges transformantes, obliques et divergentes : la marge oblique du bassin de Morondava à l’Ouest, bornée par la ride de Davie, et au Nord, la marge divergente du bassin de Majunga connectée au bassin de Somalie. Cette île de 1600 kilomètres de long est composée d’un plateau axial archéen-protérozoïque entre 1200 et 1800m d’altitude, bordé de tous côtés par des bassins sédimentaires. Le sommet du plateau correspond à des surfaces d’aplanissement altérées, délimitées par des escarpements plus ou moins marqués. L'altitude des hauts plateaux traduit l'existence de processus mantelliques, mais la cinétique et l'origine du relief malgache est mal comprise. Peu d'études ont étudié les domaines non orogéniques dans leur intégralité terre-mer, depuis le bassin versant en érosion jusqu'aux marges en sédimentation, et aucune d'entre elles ne porte sur Madagascar. Ce travail de thèse repose donc sur une double approche: une analyse géomorphologique des formes du relief (surfaces d'aplanissement) à terre, basée sur leur (i) cartographie, (ii) chronologie relative, (iii) relation avec les profils d'altération et (iv) datation au moyen des placages sédimentaires et du volcanisme daté qui les scellent; une analyse stratigraphique de l'intervalle post-rift des marges, basée sur l'interprétation de données de sub-surface (puits et lignes sismiques), lesquelles ont été réévaluées en âge (biostratigraphie), pour (i) identifier, dater et mesurer les déformations des marges et de leur relief en amont, (ii) mesurer les flux silicoclastiques, produits de l'érosion continentale. Un calendrier et une cartographie des déformations ont été obtenus sur les marges et mis en relation avec les différentes générations de surfaces d'aplanissement étagées caractérisant le relief malgache. Au Crétacé supérieur, une flexuration de l'île est initiée au sud, à grande longueur d'onde, autour de ~94 Ma. Cette déformation est scellée par la mise en place d'une surface d'aplanissement non déformée mise en place entre 80 et 66 Ma. Durant le Paléocène jusqu’à l'Eocène supérieur (66 à 20 Ma), Madagascar est une île relativement plate, de faible altitude, entourée de larges plateformes carbonatées. Ce relief est largement altéré avec la croissance de nombreux profils latéritiques et les influx silico-clastique dans les bassins sont alors relativement faibles. Le Miocène moyen à supérieur correspond au paroxysme de la surrection et de la déformation avec (1), le basculement de la marge ouest (Morondava), (2) une augmentation du flux de sédimentation silicoclastique depuis le Miocène moyen et (3) la mise en place d’une succession de quatre surfaces d’aplanissement correspondant à des pics d'intensité de la déformation. Le résultat de cette surrection est la morphologie en dôme de l’île de Madagascar (avec un plateau central) marquée par la forme concave de la surface crétacé supérieure altérée à l’Eocène. Le mécanisme de la surrection doit prendre en compte une déformation de très grande longueur d’onde (x 1000 km), forcément liée à la dynamique mantellique. Les relations avec les dômes d’Afrique de l’Est (Ethiopie, Afrique du Sud) sont discutées
Madagascar is an Archean to Neoproterozoic continental crust surrounded by transform, oblique and divergent margins: the transform Morondava basin to the west, pounded by the Davie Fracture Zone, and to the north, the divergent Mahajanga Basin connected to the Somali Oceanic Basin. This 1600 km long island is a high axial plateau with elevations from 1200 to 1800m. The top of the plateau corresponds to weathered planation surfaces (etchplains), bounded by more or less high scarps. Such elevation of the high axial plateau imply mantle processes, but the age and cinetic of the uplift is still poorly known. Few studies dealt with anorogenic domains in their entirety from the catchment area, the source, to the downstream depositional system, the sink, none of which is about Madagascar. This work lies on a double approach : it is onshore based on the analysis of the macroforms (planation surfaces, etchplains, pediments) throughout their (i) mapping, (ii) relative dating, (iii) relationships with weathering profiles and (iv) dating by their intersection with preserved sediments and volcanism (lava flow and intrusions). offshore, it is based on the interpretation of a dataset of seismic lines and industrial wells, coupled with refreshed biostratigraphy, in order to (i) identify, date and measure vertical movements of the margins and upstream reliefs. Chronology and mapping of vertical movements were defined on the Morondava margin and compared with the onset of the stepped planation surfaces typical of Madagascar topography. During Upper Cretaceous, the southern part of the island is uplifted, at ~94 Ma. This deformation is sealed by the onset of an undeformed planation surface between 80 and 66 ma. From Paleocene to Upper Eocene (66 to 20 Ma), Madagascar is a flat, low elevated island, surrounded by wide carbonate platforms. The relief is highly weathered with growth of lateritic profiles and silico-clastic influx within the basin is low. During Middle to Upper Miocene is the uplift and doming paroxysm with (1), tilt of the western margin (Morondava), (2) increase of silico-clastic influx from Middle Miocene and (3 the onset of four planation surfaces associated to deformation paroxysms. The end result of this uplift is a convex up shape pattern for the end Cretaceous surface weathered during Eocene times, creating the present-day dome morphology (with a central plateau) of Madagascar. The mechanism of this uplift has to explain a very long wavelength deformation (x1000 km) necessary due to mantle dynamics. The relationships with the other East African domes (Ethiopia, East Africa, South Africa) are discussed
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Ranarison, Solofoarilala. "Le Jurassique et le Crétacé (Callovien-Cénomanien) de la région d'Antsalova, bassin de Morondava (Madagascar) biostratigraphie, sédimentologie /." Grenoble 2 : ANRT, 1988. http://catalogue.bnf.fr/ark:/12148/cb37617888q.

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Ranarison, Solofoarilala. "Le jurassique et le crétacé (callovien - cénomanien) de la région d'Antsalova, bassin de Morondava (Madagascar) : biostratigraphie - sédimentologie." Lyon 1, 1988. http://www.theses.fr/1988LYO10169.

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Etude du bassin de morondava, madagascar. L'analyse biostratigraphique est realisee a partir des nanofossiles calcaires et des foraminiferes; les ages obtenus sont confirmes ou precises grace a l'utilisation conjointe des ammonites et belemnites. L'existence du berriasien superieur est etablie ainsi que la limite valanginien superieur-hauterivien. L'analyse sedimentologique montre la mise en place puis le developpement d'une plateforme carbonatee progradante subissant une subsidence variable dans l'espace et le temps. On reconnait 7 megasequences, elles-memes subdivisees. La comparaison des sequences et discontinuites ainsi definies avec les cycles eustatiques de 2eme ordre de haq et al. (1987) montre des dissemblances au valanginien et au cenomanien
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Ramakavelo-Ranoronirina, Marie Geneviève. "Etude micropaléontologique du crétacé supérieur et du paléogène de la région de Toliary (Tuléar) Bassin de Morondava (Madagascar)." Paris 6, 1989. http://www.theses.fr/1989PA066413.

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Dans le bassin de morondava, neuf coupes couvrant au total 600 m de sediments ont ete levees a partir de basaltes d'age campanien. Les foraminiferes benthiques et planctoniques, les ostracodes, les algues calcaires ont ete utilises pour la premiere fois pour dater les 7 formations que nous avons reconnues: (1) les calcaires a siderolites (maastrichtien), (2) les calcaires a algues de vineta (paleocene), (3) les calcaires greseux a miscellanea (paleocene), (4) les calcaires a nummulites d'ambohimahavelona (ypresien), (5) les calcaires a fabiania cassis de miary (luterien superieur-bartonien), (6) les calcaires a fabularia d'ankaiasy (bartonien-priabonien), (7) les calcaires a huitres de la table (priabonien). Des lacunes sedimentaires ont ete aussi decelees a la limite mesocenozoique, a la base de l'ypresien et celle de l'eocene moyen. Les microfacies etalonnes sur deux modeles de sedimentation de plate-forme carbonatee nous ont permis de reconstituer les milieux de depots des differentes formations. Ainsi, la sedimentation paleogene serait proche de celle que l'on connait actuellement au large de toliary. De l'extension des rudistes et de certains microorganismes rencontres au cours de cette etude (foraminiferes benthiques, ostracodes) nous avons pu etablir que la region de toliary se trouve au cretace superieur a la limite de deux zones climatiques (tropicale et temperee) et au cours du paleogene dans la tropicale
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LALAOHARIJAONA, RAMAHAVORY RASOAMBOLANORO. "Evolution de la marge ouest-malgache au jurassique : le bassin de morondava entre les fleuves tsiribihina et mangoky (madagascar)." Paris 6, 1993. http://www.theses.fr/1993PA066746.

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A partir des donnees de terrain, de subsurface (forages et geophysiques) et de la photo-interpretation, on a mis exergue l'evolution tectono-sedimentaire du bassin de morondava entre la tsiribihina et la mangoky pendant le jurassique. Les incursions marines debutent au toarcien au terme duquel on assiste a une phase d'aplanissement du bassin suivie de l'accretion des plates-formes limitee pratiquement au bajocien-bathonien. La polarit paleogeographique se presente davantage suivant une direction sse-nnw pour devenir e-w a partir du callovien periode durant laquelle les depots bassinaux commencent a se developper. Les directions tectoniques majeures (nnw-sse et nne-ssw) qui ont controle la sedimentation sont heritees des accidents responsables de la fracturation du substrat karroo. Les accidents de la famille directionnelle wnw-ese a w-e seraient de meme age que les dykes doleritiques qui les occupent (albo-cenomanien a maastrichtien). Les intumescences produites par les corps gabbroiques mis en place depuis la fin du jurassique moyen au neocomien sont a l'origine des erosions plus ou moins poussees des series jurassiques des regions affectees. Elles sont realisees avant le depot de l'albo-cenomanien. Les phenomenes tectoniques et magmatiques enregistres dans le bassin de morondava se retrouvent a travers l'evolution du canal de mozambique
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Rajaomazava, Félix. "Etude de la subsidence du bassin sédimentaire de Morondava (Madagascar) dans le cadre de l'évolution géodynamique de la marge est-africaine /." Montpellier : Centre géologique et géophysique, 1992. http://catalogue.bnf.fr/ark:/12148/cb35523404j.

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Andriamanantena, Johary. "Etudes sédimentologiques et séquentielles de la partie médiane du groupe du Karroo (Permo-Trias) de la région de Malaimbandy (Bassin de Morondava) Madagascar." Grenoble 2 : ANRT, 1987. http://catalogue.bnf.fr/ark:/12148/cb376023371.

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Books on the topic "Morondava"

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Rajaomazava, Félix. Etude de la subsidence du bassin sédimentaire de Morondava (Madagascar): Dans le cadre de l'évolution géodynamique de la marge est-africaine. Montpellier, France: Centre géologique et géophysique, Université des sciences et techniques du Languedoc, 1992.

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Kolikoly, Fanoitra Miady Amin'ny. Tahirin-kevitra ho an'ny fametrahana tambazotran'ny fiarahamonim-pirenena miady amin'ny kolikoly isam-paritra: Antananarivo-- Antsirabe--Antsiranana--Maintirano--Mahajanga--Morondava--Sambava--Taolagnaro--Toamasina--Toliara. [Antananarivo]: UNDP, 2005.

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(Madagascar), Observatoire national du secteur forestier. Rapports de mission de L'OSF: À Didy Ambatondrazaka (22/06 au 25/06/05), à Antalaha (02/07 au 05/07/05), à Morondava (20/05 au 28/05/05), à Tuléar (10/08 au 13/08 et 23/08 au 03/09/05). Antananarivo: Observatoire national du secteur forestier, 2005.

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Book chapters on the topic "Morondava"

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Wright, R. P., and R. A. Askin. "The Permian-Triassic Boundary in the Southern Morondava Basin of Madagascar as Defined by Plant Microfossils." In Gondwana Six: Stratigraphy, Sedimentology, and Paleontology, 157–66. Washington, D. C.: American Geophysical Union, 2013. http://dx.doi.org/10.1029/gm041p0157.

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Conference papers on the topic "Morondava"

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Shi, K., and Z. Guo. "The Hydrocarbon Prospectivity of the Offshore Morondava Basin, Madagascar." In First EAGE Eastern Africa Petroleum Geoscience Forum. Netherlands: EAGE Publications BV, 2015. http://dx.doi.org/10.3997/2214-4609.201414463.

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S. Tamannai, M., D. Winstone, I. Deighton, and P. Conn. "An Evaluation of the Petroleum System - Offshore Morondava Basin, Madagascar, Based on 2D Seismic Data Interpretation." In 70th EAGE Conference and Exhibition - Workshops and Fieldtrips. European Association of Geoscientists & Engineers, 2008. http://dx.doi.org/10.3997/2214-4609.20147564.

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