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Reassessment of local earthquake data from the ANCORP seismological network allowed the calculation of 3D attenuation (Q(p)) tomographic images of crust and upper mantle beneath the southern Bolivian Altiplano around 21degrees S. The images reveal a low-Q(p) middle and lower crust and a moderate-Q(p) upper mantle beneath the southern Altiplano. Beneath the recent magmatic arc, Q(p) is not significantly decreased at this latitude. The distribution of crustal Q(p) coincides with the variation of electrical resistivity, thus limiting the possible mechanisms causing the anomalies. Our findings support the hypothesis that partial melts in middle and lower crust beneath the Altiplano are present on a large scale. We see no evidence for a shallow asthenosphere beneath the southern Altiplano
Seismic tomography, imaging of seismic scatterers, and magnetotelluric soundings reveal a sharp lithologic contrast along a similar to 10 km long segment of the Arava Fault (AF), a prominent fault of the southern Dead Sea Transform (DST) in the Middle East. Low seismic velocities and resistivities occur on its western side and higher values east of it, and the boundary between the two units coincides partly with a seismic scattering image. At 1 - 4 km depth the boundary is offset to the east of the AF surface trace, suggesting that at least two fault strands exist, and that slip occurred on multiple strands throughout the margin's history. A westward fault jump, possibly associated with straightening of a fault bend, explains both our observations and the narrow fault zone observed by others
The whereabouts of the Balaenoptera borealis holotype, the skeleton of a 1819 stranded specimen, have been unknown since the World War II (WWII). Due to nomenclatural confusion, deficient documentation, and finally WWII bombing, which destroyed predominantly cetacean material in the Museum fib Naturkunde Berlin (MfN), the type skeleton of the sei whale sank into oblivion. Construction activities enabled a recent search and study on the remaining whale material. Here, we provide evidence that the type specimen was not destroyed. On the basis of species-wide and individual characters of the type material such as the shape of cranial elements and the pattern of the maxillary foramina, we show that the skull and mandibles, the vertebral column (except the atlas), and the ribs of the holotype remain intact. Further evidence that these skeletal remains belong to the previously missing holotype is provided by the characteristics of the spine. In addition, we analyzed ancient DNA from bone samples and confirm they are B. borealis, and the occurrence of same mitochondrial haplotypes indicate that the bones belong to the same individual. Additionally, a blue inscription was discovered at the caudal epiphysis of a thoracic vertebra; historical research matched this inscription with the material belonging to the former Anatomical-Zootomical Museum, from which the holotype was once bought.
Fault zones are the locations where motion of tectonic plates, often associated with earthquakes, is accommodated. Despite a rapid increase in the understanding of faults in the last decades, our knowledge of their geometry, petrophysical properties, and controlling processes remains incomplete. The central questions addressed here in our study of the Dead Sea Transform (DST) in the Middle East are as follows: (1) What are the structure and kinematics of a large fault zone? (2) What controls its structure and kinematics? (3) How does the DST compare to other plate boundary fault zones? The DST has accommodated a total of 105 km of left-lateral transform motion between the African and Arabian plates since early Miocene (similar to 20 Ma). The DST segment between the Dead Sea and the Red Sea, called the Arava/Araba Fault (AF), is studied here using a multidisciplinary and multiscale approach from the mu m to the plate tectonic scale. We observe that under the DST a narrow, subvertical zone cuts through crust and lithosphere. First, from west to east the crustal thickness increases smoothly from 26 to 39 km, and a subhorizontal lower crustal reflector is detected east of the AF. Second, several faults exist in the upper crust in a 40 km wide zone centered on the AF, but none have kilometer-size zones of decreased seismic velocities or zones of high electrical conductivities in the upper crust expected for large damage zones. Third, the AF is the main branch of the DST system, even though it has accommodated only a part (up to 60 km) of the overall 105 km of sinistral plate motion. Fourth, the AF acts as a barrier to fluids to a depth of 4 km, and the lithology changes abruptly across it. Fifth, in the top few hundred meters of the AF a locally transpressional regime is observed in a 100-300 m wide zone of deformed and displaced material, bordered by subparallel faults forming a positive flower structure. Other segments of the AF have a transtensional character with small pull-aparts along them. The damage zones of the individual faults are only 5-20 m wide at this depth range. Sixth, two areas on the AF show mesoscale to microscale faulting and veining in limestone sequences with faulting depths between 2 and 5 km. Seventh, fluids in the AF are carried downward into the fault zone. Only a minor fraction of fluids is derived from ascending hydrothermal fluids. However, we found that on the kilometer scale the AF does not act as an important fluid conduit. Most of these findings are corroborated using thermomechanical modeling where shear deformation in the upper crust is localized in one or two major faults; at larger depth, shear deformation occurs in a 20-40 km wide zone with a mechanically weak decoupling zone extending subvertically through the entire lithosphere.