S. E. Wilmer and Audrone Zukauskaite. Interrogating Antigone in Postmodern Philosophy and Criticism. Oxford, Oxford University Press. 2010 pp: ix + 448

Fil: Saravia de Grossi, María Inés. Universidad Nacional de La Plata. Facultad de Humanidades y Ciencias de la Educación. Instituto de Investigaciones en Humanidades y Ciencias Sociales (UNLP-CONICET); Argentina.

El prólogo de Áyax : Un compendio del arte dramático de Sófocles

Este estudio considera que en el Prólogo de Áyax se encuentran las características fundamentales del teatro de Sófocles, como lo ha afirmado Lesky en 'Sophokles und Das Humane'. Se enumeran las pautas que el crítico considera más relevantes del pensamiento del autor y se las analiza en la primera escena de la obra. Finalmente, se expresan las conclusiones

El discurso de Polinices (vv. 1284-1345) en Edipo en Colono de Sófocles

Edipo en Colono de Sófocles resulta una obra fuertemente argumentativa por los debates dialécticos que se presentan entre los Episodios II a IV, cuya función dramática consiste en demorar el destino de Edipo y, a su vez, desplegar una densidad intratextual muy rica. Easterling (1999: 95-107) afirma que hay tres rasgos que definen el estilo de Sófocles, ellos son, por un lado, la tensión de opuestos o contradicciones; en segundo lugar, la oscilación entre el sentido literal y el sentido metafórico y, por último, la concentración junto con el uso de repeticiones. En el presente estudio analizamos el discurso de Polinices como el ejemplo de las características mencionadas, las que convierten la intervención del joven guerrero en el punto cultimante de las escenas agonales, que constituyen el núcleo de la obra. Estas instancias disonantes que los enfrentamientos producen son atemperadas por la presencia de Teseo.

Las manifestaciones de "filía" y conceptos vinculados en Edipo en Colono de Sófocles

Fil: Saravia de Grossi, María Inés. Universidad Nacional de La Plata. Facultad de Humanidades y Ciencias de la Educación. Instituto de Investigaciones en Humanidades y Ciencias Sociales (UNLP-CONICET); Argentina.

Nannofossil assemblages and flux rates during the late Oligocene-early Miocene

This study investigates abundance variations in Noelaerhabdaceae assemblages during the late Oligocene-early Miocene at three subtropical sites in the Atlantic and Pacific oceans (DSDP Sites 516, 608 and 588). At these three sites, nannofossil assemblages were characterized by the successive high proportion of Cyclicargolithus, Dictyococcites and Reticulofenestra. Local paleoceanographic changes, such as the input of nutrient-poor water masses, might explain shifts in ecological prominence within the Noelaerhabdaceae at DSDP Site 516 (South Atlantic). But the similar timing of a decline in Cyclicargolithus at the three studied sites more likely corresponds to a global process. Here, we explore possible causes for this long-term taxonomic turnover. A global change in climate, associated with early Miocene glaciations, could have triggered a decline in fitness of the taxon Cyclicargolithus. The ecological niche made vacant because of the decrease in Cyclicargolithus could then have been exploited by Dictyococcites and Reticulofenestra that became prominent in the assemblages after 20.5 Ma. Alternatively, this global turnover might reflect a gradual evolutionary succession and be the result of other selection pressures, such as increased competition between Cyclicargolithus and Dictyococcites/Reticulofenestra. A diversification within Dictyococcites/Reticulofenestra, indicated by an expansion in the size variation within this group since ~ 20.5 Ma, may have contributed to the decreased fitness of Cyclicargolithus.

Neptunian dikes and their fillings in carbonates of the Warstein area (northeastern Rhenish massif)

Neptunian dikes and cavities as weil as their fillings are described from Middle to Upper Devonian carbonates of the Warstein area. The genesis of the pre-Upper Carboniferous dikes is due to pre-orogenic synsedimentary tensional movements. Lifting, subsidence and tilting caused joints and cracks, which are enlarged to dikes and cavities on submarine conditions. The post-Upper Carboniferous dikes are based on the orogenesis during Upper Carboniferous time, causing numerous tectonical divisional planes in the sediments. Along these planes a far-reaching karstification took place since mesozoic time. According to their size the cavities are subdivided into macro-, mega- and microdikes. With the exception of one macrodike all the others are limited to the massive limestone. Megadikes especially occur in Upper Devonian cephalopod limestone and in the Erdbach limestone, microdikes can be found in all carbonatic rocks. The dikes follow pre-orogenic, tectonical and sedimentary divisional planes and are orientated to ac-, bc- as well as bedding planes and diagonal directions. The fillings happened down from above either in a solitary event or repeatedly in long-lived dikes during a span of several ten millions of years. More seldom the fillings took place laterally or upside from beneath. The dikes contain - without regard to autochthonous conodont faunas - older and/or younger mixed faunas, too. Occasionally they were used as life district by a trilobite fauna adapted to the dikes. The dikes represent sedimentary pitfalls and conserve sediments eroded in other places. Therefore, by aid of the fillings, it can be demonstrated, that stratigraphic gaps are not absolutely due to primary interruptions of sedimentation, but were caused by reworking. Some dikes contain the distal offsets of slides and suspension streams. Relations between condensation and development of dikes could not be derived in the Warstein area. However, an increase of the frequency of dikes towards east to the eastern margin of the Warstein carbonate platform could be pointed out. This margin is a slope, persisting more than 10 millions of years, between a block and a basin. Evidently cracks and dikes, which were caused by settlements, slides and earth quakes, occured there frequently. The Warstein dikes and cavities, caused by karstification, are filled with terrestrial Lower Cretaceous, marine Upper Cretaceous and terrestrial Pleistocene to Holocene sediments. Tertiary sediments could not be detected.