Datos paleomagnéticos del sustrato rocoso de la isla de Livingston (Península Antártica): implicaciones tectónicas en la evolución neógena

We report paleomagnetic results from the Miers Bluff Formation and Tertiary dykes and andesites in Livingston Island (South Shetland Islands, Antarctic Peninsula). Most of the samples carry stable magnetization, residing in a low coercivity phase, most likely (Ti)magnetite. Progressive untilting of the Characteristic Remanent Magnetization directions reveals that the magnetization of the turbidites (Miers Bluff Fm.) is post-folding. Miers Bluff and the dyke mean directions do not show any significant difference, suggesting the same magnetization age. Thus, a local Cenozoic remagnetization is proposed. Also, the paleomagnetic poles suggest a tectonic tilting that would explain the observed discrepancies between the produced paleopoles and the APWP for the Antarctic Peninsula

Datos paleomagnéticos del sustrato rocoso de la isla de Livingston (Península Antártica): implicaciones tectónicas en la evolución neógena

Se presentan resultados paleomagnéticos de la Fo rmación Miers Bluff y de los diques terciarios y andesitas de la Isla de Livingston (Islas Shetland del Sur, Península A n t á rtica). La mayoría de las rocas estudiadas son portadoras de magnetización estable, que reside en una fase de baja coercividad, probablemente Ti-Magnetita. La restitución tectónica progresiva de las direcciones de magnetización remanente característica revela que la magnetización en las turbiditas de la Fm. Miers Bluff fue adquirida después del plegamiento. Las direcciones medias de los diques y de la Fm. Miers Bluff no ofrecen una diferencia significativa, sugiriendo una misma edad para la magnetización. Se propone que el origen de la misma es una remagnetización de edad terciaria. Asimismo, la posición de los polos paleomagnéticos obtenidos sugiere un basculamiento tectónico que estaría relacionado con la apertura y extensión en el Estrecho de Bransfield.We report paleomagnetic results from the Miers Bluff Formation and Tertiary dykes and andesites in Livingston Island (South Shetland Islands, Antarctic Peninsula). Most of the samples carry stable magnetization, residing in a low coercivity phase, most likely (Ti)magnetite. Progressive untilting of the Characteristic Remanent Magnetization directions reveals that the magnetization of the turbidites (Miers Bluff Fm.) is post-folding. Miers Bluff and the dyke mean directions do not show any significant difference, suggesting the same magnetization age. Thus, a local Cenozoic remagnetization is proposed. Also, the paleomagnetic poles suggest a tectonic tilting that would explain the observed discrepancies between the produced paleopoles and the APWP for the Antarctic Peninsula

Proposed Global Stratotype Sections and Points for the bases of the Selandian and Thanetian stages (Paleocene Series)

Prepared for the International Subcommission on Paleogene Stratigraph

Paleomagnetic dating of non-sulfide Zn-Pb ores in SW Sardinia (Italy): a first attempt

A first paleomagnetic investigation aimed at constraining the age of the non-sulfide Zn-Pb ore deposits in the Iglesiente district (SW Sardinia, Italy) was carried out. In these ores, the oxidation of primary sulfides, hosted in Cambrian carbonate rocks, was related to several paleoweathering episodes spanning from the Mesozoic onward. Paleomagnetic analyses were performed on 43 cores from 4 different localities, containing: a) non-oxidized primary sulfides and host rock, b) oxidized Fe-rich hydrothermal dolomites and (c) supergene oxidation ore («Calamine»). Reliable data were obtained from 18 samples; the others show uninterpretable results due to low magnetic intensity or to scattered demagnetization trajectories. Three of them show a scattered Characteristic Remanent Magnetization (ChRM), likely carried by the original (i.e. Paleozoic) magnetic iron sulfides. The remaining 15 samples show a well defined and coherent ChRM, carried by high-coercivity minerals, acquired after the last phase of counterclockwise rotation of Sardinia (that is after 16 Myr), in a time interval long enough to span at least one reversal of the geomagnetic field. Hematite is the main magnetic carrier in the limestone, whereas weathered hydrothermal dolomite contains goethite or a mixture of both. The results suggest that paleomagnetism can be used to constrain the timing of oxidation in supergene-enriched ores

A 1-Million-Year Record of Environmental Change in the Central Mediterranean Sea From Organic Molecular Proxies

The Mediterranean Sea is particularly sensitive to climate oscillations and represents a key location to study past climatic and oceanographic changes. One valuable source of paleoceanographic information is through molecular biomarkers in deep sea sediments. This approach has been applied in a number of studies in this basin, but only covering the most recent glacial/interglacial cycles. Here we present, for the first time in the Mediterranean Sea, a molecular biomarker record from the Strait of Sicily that covers the last million years until the present, almost continuously. We present data on alkenone derived urn:x-wiley:25724517:media:palo21102:palo21102-math-0001 index sea surface temperatures (SST) and provide insights on the evolution of the phytoplankton community composition and terrestrial inputs through the analysis of the concentrations of alkenones, brassicasterol and long-chain alcohols. The urn:x-wiley:25724517:media:palo21102:palo21102-math-0002-SST record followed a climatic evolution modulated by glacial/interglacial cycles with a marked increase in the 100 kyr-amplitude of the glacial cycles at ∼430 ka, coincident with the Mid-Brunhes transition. In addition, SSTs were consistently higher compared with other records in the western Mediterranean, indicative of the progressive warming that surface waters experience along their transit from the Strait of Gibraltar to the Central Mediterranean. Regarding the concentrations of alkenones and brassicasterol, they displayed distinct alternate peaks, some of them coeval with the deposition of sapropels. This suggests that different environmental and oceanographic conditions characterized each sapropel which, together with changes in terrestrial inputs and the degree of oligotrophy, induced the alternate proliferation of coccolithophores and diatoms.Postprin

FIELD TRIP TO THE YPRESIAN/LUTETIAN BOUNDARY AT THE GORRONDATXE BEACH SECTION (BASQUE COUNTRY, W PYRENEES)

One of the Paleogene Stage boundaries still needing official definition is the Ypresian/Lutetain (Early- Middle Eocene) boundary. With the aim of contributing to attain this definition, a high-resolution multidisciplinary study, including physical stratigraphy (lithostratigraphy, sequence stratigraphy and magnetostratigraphy) and biostratigraphy (calcareous nannofossil, planktic foraminifer and larger foraminifer), has been carried out over the 700 m thick uppermost Ypresian – lower Lutetian Gorrondatxe section. The results show that the different events traditionally used to place the Ypresian/Lutetian boundary, hitherto thought to be simultaneous (i.e., the planktic foraminifer P9 (=E7) / P10 (=E8) Zone boundary; the calcareous nannofossil CP12a / CP12b Subzone boundary; the larger foraminifer SBZ12 / SBZ13 Zone boundary; and the boundary between magnetic polarity chrons C22n and C21r), actually occur at very different levels. Therefore, before considering any section to place the Ypresian/Lutetian boundary stratotype, the criterion to precisely define this boundary should be selected. To this end, the succession of events pinpointed in the Ypresian/Lutetian boundary interval of the Gorrondatxe beach section might prove a useful database. The Gorrondatxe section fulfils most of the requirements demanded of a prospective stratotype section. In addition, the great sedimentary thickness, which implies a very high deep-marine sedimentation rate, provides the Gorrondatxe section an additional value, as it offers the opportunity to chronologically order successive biomagnetostratigraphic events more precisely than elsewhere. Therefore, we consider that, once the criterion to define the Ypresian/Lutetian boundary is selected, the Gorrondatxe beach section should be deemed a firm candidate to place the Global Stratotype Section and Point of the base of the Lutetian Stage

Correlation of the Thanetian-Ilerdian turnover of larger foraminifera and the Initial Eocene thermal maximum (IETM) confirming evidence from the Campo area (Pyrenees, Spain)

Abstrac

Cyclostratigraphy of the Early/Middle Eocene transition: a Pyrenean perspective

An integrated bio-, magneto- and cyclostratigraphic study of the Ypresian/Lutetian (Early/Middle Eocene) transition along the Pyrenean Otsakar section (Payros et al., 2011) resulted in the identification of the C22n/C21r chron boundary and of the calcareous nannofossil CP12a/b zonal boundary; the latter is the main correlation criterion of the Lutetian Global Stratotype Section and Point (GSSP) recently defined at Gorrondatxe (Basque Country). By counting precession-related mudstone-marl couplets of 21 ka, the time lapse between both events was calculated to be of 819 ka. This suggests that the age of the CP12a/b boundary, and hence that of the Early/Middle Eocene boundary, is 47.76 Ma, 250 ka younger than previously thought. This age agrees with, and is supported by, estimates from Gorrondatxe based on the time lapse between the Lutetian GSSP and the C21r/C21n boundary. The duration of Chron C21r is estimated at 1.326 Ma. Given that the base of the Eocene is dated at 55.8 Ma, the duration of the Early Eocene is of 8 Ma, 0.8 Ma longer than in current time scales. The Otsakar results further show that the bases of planktic foraminiferal zones E8 and P10 are younger than the CP12a/b boundary. The first occurrence of Turborotalia frontosa, being approximately 550 ka older that the CP12a/b boundary, is the planktic foraminiferal event that lies closest to the Early/Middle Eocene boundary. The larger foraminiferal SBZ12/13 boundary is located close to the CP12a/b boundary and correlates with Chron C21r, not with the C22n/C21r boundary