5 documents found in 110ms
# 1
Thybo, Hans • Balling, Niels • Maupin, Valerie • Ritter, Joachim • Tilmann, Frederik
Abstract: The ScanArray experiment is a major collaborative effort of institutions in Scandinavia and Germany to map crustal and mantle structure below Scandinavia using a dense temporary deployment of broadband seismometers. Scientific questions to be addressed include (among others): 1. What supports the topographic high of the Scandes? 2. How does lithospheric thickness vary within Fennoscandia? 3. What is the internal fabric of the mantle lithosphere? 4. Are there differences in the crustal structure between the different blocks of Fennoscandia? This data set, termed ScanArray core, comprises the temporary stations deployed by the University of Copenhagen, the University of Aarhus, and the University of Oslo, the Karlsruhe Institute of Technology (KIT) and the GeoForschungsZentrum Potsdam (GFZ) as part of the ScanArray experiment. Stations within this dataset are deployed for periods between 2 and 4 years. Data are available from the GFZ seismological data archive with network code 1G. Waveform data will be fully opened in early 2020. The wider ScanArray dataset additionally includes the multi-use temporary deployments Neonor2 (FDSN-code 2D, University of Bergen, NORSAR) and ScanLips3D (University of Leicester; archived at IRIS DMC), and the permanent networks of Sweden (UP, SNSN), Norway (NS, NNSN), Denmark (DK, DNSN) and Finland (HE, FNSN) as well as a subset of NORSAR stations (NO). The SNSN rearranged the distribution of broadband seismometers and deployed additional temporary stations to meet the objectives of the ScanArray experiment. ScanArray core and these other networks (except ScanLips3D) jointly form the virtual network _SCANARRAY. Partners of the ScanArray consortium are: University of Aarhus, Uppsala University, University of Oslo, University of Bergen, Karlsruhe Institute of Technology, NORSAR, University of Copenhagen, Deutsches GeoForschungsZentrum (GFZ) and Istanbul Technical University.
# 2
Schurr, Bernd • Yuan, Xiaohui • Haberland, Christian • Mechie, James • Kufner, Sofia-Katerina
Abstract: The TIPTIMON seismic deployment in Tajikistan aimed to study the seismotectonics of the western Pamir and Tajik-Afghan basin. Within this network 25 seismic stations were deployed between 2012 to 2014 to study shallow and intermediate depth seismicity. TIPTIMON (Tien Shan-Pamir Monitoring) is a research programme funded by the German Federal Ministry of Education and Research (BMBF) within the CAME Programme (Central Asia - Monsoon dynamics and Geo-ecosystems). All stations recorded continuously with 100 samples per second and were equipped with EDL (EarthData PR6-24) recorders and broadband seismometers. Waveform data is available from the GEOFON data centre, under network code 5C, and is embargoed until April 2018.
# 3
Qian, Hui • Mechie, James
Abstract: From June 2012 to November 2013, the Chinese Academy of Geological Sciences (CAGS) together with the Deutsches GeoForschungsZentrum Potsdam (GFZ) operated an array of 80 broadband seismic stations in a 300 km by 150 km area straddling the Longmenshan fault zone around the epicentre of the Wenchuan earthquake. Since the occurrence of the Ms 8.0 Wenchuan earthquake which ruptured about 300 km of the Longmenshan fault zone in May 2008, this region has attracted the attention of many Earth scientists. Since the earthquake the Wenchuan Earthquake Fault Scientific Drilling (WFSD) Project has drilled several holes up to 3 km depth. The main purpose of the present array of seismological stations is to investigate the deep structure of the region surrounding the epicentre of the Wenchuan earthquake. While the array was operating the Ms 6.6 Lushan earthquake occurred in April 2013 at the SW edge of the array. Waveform data is available from the GEOFON data centre, under network code 2F, and is embargoed until DEC 2017.
# 4
Tilmann, Frederik • Yuan, Xiaohui • Rümpker, Georg • Rindraharisaona, Elisa
Abstract: The island of Madagascar occupies a key region in both the assembly and the multi-stage breakup of Gondwanaland, itself part of the super-continent Pangaea. Madagascar consists of an amalgamation of continental material, with the oldest rocks being of Archaean age. Its ancient fabric is characterised by several shear zones, some of them running oblique to the N-S trend, in particular in the south of the island. More recently during the Neogene, moderate volcanism has occurred in the Central and Northern part of the island, and there are indications of uplift throughout Eastern Madagascar over the last 10 Ma. Although Madagascar is now located within the interior of the African plate and far away from major plate boundaries (>1000 km from the East African rift system and even further from the Central and South-West Indian Ridges), its seismic activity indicates that some deformation is taking place, and present-day kinematic models based on geodetic data and earthquake moment tensors in the global catalogues identify a diffuse N-S-oriented minor boundary separating two microplates, which appears to pass through Madagascar. In spite of the presence of Archaean and Proterozoic rocks continent-wide scale studies indicate a thin lithosphere (<120 km) throughout Madagascar, but are based on sparse data and cannot resolve the difference between eastern and western Madagascar. We have operated an ENE-WSW oriented linear array of 25 broadband stations in southern Madagascar, extending from coast to coast and sampling the sedimentary basins in the west as well as the metamorphic rocks in the East, cutting geological boundaries seen at the surface at high angle. The array crosses the prominent Bongolava-Ranotsara shear zone which is thought to have been formed during Gondwanaland assembly. The array recorded the magnitude 5.3 earthquake of January 25, 2013 which occurred just off its western edge. In addition, in May 2013 we have deployed 25 short period sensors in the eastern part of the study area, where there is some so-far poorly characterised seismicity. Waveform data is available from the GEOFON data centre, under network code ZE, and is embargoed until DEC 2018.
# 5
Passarelli, Luigi • Roessler, Dirk • Aladino, Govoni • Maccaferri, Francesco • Moretti, Milena • (et. al.)
Abstract: The temporary Pollino Seismic Experiment, FDSN network code 4A, monitored the earthquake swarm in the Pollino Range region, Italy, between November 2012 and September 2014. The region is located at the transition from the Southern Apennines chain to the Calabrian arc. Striking a volume of about 20x20x15 km, the swarm started in October 2010, culminated in an Mw=5.2 event on 25 October 2012, and has continued since with a variable rate of activity. The area represents a seismic gap as there are no documented historical M>6 earthquakes during the last thousand years. The tectonic structures of the area are poorly known. The experiment was part of a collaborative effort made by the German Research Centre for Geosciences (GFZ) and the Istituto Nazionale di Geofisica e Vulcanologia (INGV) within the framework of the NERA and CCMP-Pompei projects. The 4A network consisted of 9 stations including 6 short-period and 3 broadband instruments, provided by GFZ. The permanent seismic network was complemented by the 9 GFZ stations and 5 IV stations temporarily installed by INGV. The short-period stations had Mark L-4C3D sensors with EDL digitizers. The broadband stations were equipped with STS2.5 seismometers and RefTek RT130S digitizers. Five short period and one broadband (CSA0 to CSA5) were installed in a small-aperture array in the west of the range. The other three stations (broadband: CSB, CSC and short period: CSD) were installed around the swarm area. The array and the network stations recorded in continuous mode at 200 Hz and at 100 Hz, respectively. The sensors were buried in the ground at 0.5 m depth except for CSB and CSD which were installed on the surface. High-precision station coordinates were obtained by using differential GPS measurements. The data have been used to analyze the earthquakes and seismogenetic structures and to discern the characteristics of the swarm sequence.
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