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Sedimentology, Biostratigraphy and Mineralogy of the Lercara Formation (Triassic, Sicily) and Its Palaeogeographic Implications

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Sedimentology, Biostratigraphy and Mineralogy of the Lercara Formation (Triassic, Sicily) and Its Palaeogeographic Implications UNIVERSITE DE GENEVE FACULTE DES SCIENCES Département de Géologie et Paléontologie Docteur R. Martini Sedimentology, Biostratigraphy and Mineralogy of the Lercara Formation (Triassic, Sicily) and its palaeogeographic implications THESE présentée à la Faculté des sciences de l’Université de Genève pour obtenir le grade de Docteur ès sciences, mention Sciences de la Terre par Lucia CAR C IONE de Longi (Italie) Thèse N° 3841 GENEVE Atelier de reproduction de la Section de Physique 2007 ai miei genitori, Lina e Pippo, con affetto. iii ABSTR A CT This thesis contributes to the resolution of one of the most controversial open questions about Sicilian geology: the age of the Lercara Formation. During the last century, it was variously attributed to the Permian, the Triassic, the Paleogene or the Miocene. A part from the question of the age, this work analyses the palaeoenvironmental context associated to the Lercara Formation deposition and the palaeogeographical evolution of the occidental part of the Tethys during the Permian and the Triassic. The study integrates sedimentological, biostratigraphic and mineralogical analyses, and proposes the reconstitution of the Sicanian basin subsidence history. The Lercara Formation deposited at the bottom of the Sicanian basin and constitutes the oldest formation cropping out in the Siculo-Maghrebian belts chain. It outcrops in western Sicily in the Roccapalumba- Lercara and Margana-Valle Riena areas, near Palazzo Adriano where it is better known as “Fiume Sosio deposits”, and in Portella Rossa near the village of Burgio. For this study, every known outcrop has been sampled, along with a new outcrop located in Portella Rossa. This field did not permit the recognition of any stratigraphic contact with the underlying formation or the basement, nor with the overlying Mufara Formation. The Lercara Formation’s main characteristic is its high content of reworked material (ca. 95%), proved by all investigation methods, particularly biostratigraphy. This material comes from the dismantlement of Permian and Triassic (Anisian) carbonate platforms and of Lower Triassic siliciclastic platforms. It is associated to ca. 5% of upper Ladinian – Cordevolian autochthonous material. This reworking explains why the age of the Lercara Formation remained unresolved for so long. The sedimentological study showed the presence of two members in the Lercara Formation: the Member A, constituted of clayey sandstones and the Member B, constituted of quartz-rich clays (B1). The Member B contains intercalated levels of either calcirudites/calcarenites (B2) or clayey sandstones (B3). Analysis of the microfacies and their spatial distribution revealed two distinct detritic sources. The main one was localised to the north-west of the Sicanian basin, while the second one was located to the south-west or the north-east. The best biostratigraphic resolution was provided by palynomorphs and foraminifers, which indicated an Anisian-Cordevolian age for the Lercara Formation. More precisely, Member A was deposited during part of the Anisian-Ladinian interval and Member B during the Ladinian-Cordevolian. Clay minerals, associated to thermal maturity indicators and to microfacies, allowed the characterisation and the differentiation of the outcrops of the Roccapalumba-Lercara, of Palazzo Adriano and of Portella Rossa areas. The Roccapalumba-Lercara sections are more proximal and underwent a higher burial loading than the Palazzo Adriano sections, which in turn are more proximal and underwent a higher burial loading than those of the Portella Rossa ones. Sedimentological and biostratigraphic data, associated to the Sicanian basin burial history, indicate that the Lercara Formation was deposited in the Neo-Tethys. This ocean was profound enough during the Middle Permian to permit the circulation of deep and cold waters. It coexisted with the Palaeo-Tethys Ocean in the Tethys western end, in a Pangea B configuration. The Sicanian basin constituted an arm of the Neo-Tethys Ocean, which from the Ladinian was separated from the Imerese basin by the proto- Vicarese carbonate platform. v RÉSUMÉ Cette thèse contribue à la résolution d’une problématique majeure de la géologie sicilienne : l’âge de la Formation Lercara. Pendant le siècle dernier, cette Formation a été assignée au Permien, au Trias, au Paleogène et au Miocène. En plus de l’âge, ce travail analyse le contexte paléo-environnemental dans lequel la formation s’est déposée et l’évolution paléogéographique de la portion occidentale de la Téthys pendant le Permien et le Trias. L’étude intègre des analyses sédimentologiques, biostratigraphiques et minéralogiques, et elle propose la reconstitution de l’histoire de la subsidence du basin Sicanien. La Formation Lercara s’est déposée dans le bassin Sicanien et constitue la plus ancienne formation sédimentaire affleurant dans la chaîne siculo-magrébine. Elle affleure dans la Sicile occidentale dans les régions de Roccapalumba-Lercara et Margana-Valle Riena, proche de Palazzo Adriano, ou elle est mieux connue comme “dépôts du Fiume Sosio”, et à Portella Rossa proche du village de Burgio. Tous les affleurements connus de la Formation Lercara ont été échantillonnés, ainsi qu’un nouveau localisé à Portella Rossa. Compte tenu de sa nature lithologique et de la tectonique intense qui affecte la Sicile, l’étude de terrain n’a jamais permis de mettre en évidence ni le contact stratigraphique inférieur avec une autre formation ou avec le socle, ni celui supérieur avec la Formation Mufara. La caractéristique fondamentale de la Formation Lercara est son contenu élevé de matériel remanié (environ 95%), mis en évidence par les différents outils utilisés, particulièrement la biostratigraphie. Ce matériel provient du démantèlement de plateformes carbonatées permiennes et triasiques (Anisien) et de plateformes siliciclastiques du Trias inférieur. Il est associé a environ 5% de matériel autochtone du Ladinien supérieur-Cordevolien. Ce remaniement très important explique pourquoi l’âge de la Formation Lercara est resté non résolu pendant si longtemps. L’étude sédimentologique a permis de distinguer deux membres dans la Formation Lercara: un Membre A constitué de grès argileux et un Membre B constitué d’argiles avec un contenu élevé en quartz. Dans le Membre B se trouvent intercalés soit des niveaux de grès argileux, soit des niveaux calciruditiques ou calcarénitiques. L’analyse des microfacies et de leur distribution spatiale a permis l’identification de deux sources d’apport détritique. La principale était probablement localisée au nord-ouest du bassin Sicanien, tandis que la seconde pouvait être localisée soit au sud-ouest, soit au nord-est. La meilleure résolution biostratigraphique a été fournie par les palynomorphes et par les foraminifères. Ils ont permis d’assigner la Formation Lercara à l’Anisien-Cordevolien. En particulier, le Membre A s’est déposé pendant une partie de l’intervalle Anisien-Ladinien et le Membre B pendant le Ladinien- Cordevolien. L’étude des minéraux argileux associée aux indicateurs de maturité thermique, ainsi que l’étude des microfacies, ont permis de caractériser et différencier les affleurements de la région de Roccapalumba- Lercara, de Palazzo Adriano et de Portella Rossa. En effet, les sections de Roccapalumba-Lercara sont plus proximales et ont subi une charge d’enfouissement plus élevée que les coupes de Palazzo Adriano, qui à leur tour sont plus proximales et ont subi une plus importante charge d’enfouissement que celles de Portella Rossa. vii Les données sédimentologiques et biostratigraphiques associées à l’histoire de subsidence du bassin Sicanien indiquent que la Formation Lercara s’est déposée dans la Néo-Téthys. Cet océan était déjà assez profond pendant le Permien moyen pour permettre la circulation d’eaux profondes et froides. Il coexistait avec l’océan Paléo-Téthysien dans la terminaison occidentale de la Téthys dans une configuration Pangea B. Le bassin Sicanien constituait un bras de la Néo-Téthys qui à partir du Ladinien, était séparé du bassin Imerese par la plateforme carbonatée proto-Vicarese. viii RI A SSUNTO La presente tesi contribuisce alla risoluzione di una delle problematiche più controverse ed ancora aperte della geologia siciliana riguardanti l’età della Formazione Lercara. Essa ha da sempre interessato i geologi perché è l’unica formazione affiorante in Sicilia a contenere una flora e una fauna permiane. Il suo studio ha dato adito negli ultimi cento anni a numerose controversie riguardo la sua età, infatti è stata assegnata al Permiano, al Trias, al Paleogene ed al Miocene. Oltre all’età, in questo studio è stato analizzato il contesto paleoambientale in cui la formazione si è deposta e la situazione geologica relativa all’evoluzione paleogeografica della porzione occidentale della Tetide durante il Permiano ed il Trias. Tutto ciò è stato realizzato grazie all’integrazione di indagini sedimentologiche, biostratigrafiche e mineralogiche, associate alla ricostruzione della storia di subsidenza del bacino Sicano. La Formazione Lercara si è deposta nel bacino Sicano e costituisce la più antica formazione affiorante nella catena siculo-magrebide. Essa affiora nelle Sicilia occidentale nelle zone di Roccapalumba- Lercara e Margana-Valle Riena, vicino Palazzo Adriano, dove è meglio conosciuta come “depositi del Fiume Sosio”, ed a Portella Rossa vicino Burgio. In campagna non sono stati riconosciuti ne il contatto stratigrafico inferiore con un’altra formazione o con il basamento, ne quello superiore
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