Important findings expected from Europe's largest seismic array

Gregersen, Søren; Pedersen, Laust B.; Roberts, Roland; Shomali, Hossein; Berthelsen, A.; Thybo, Hans; Mosegaard, Klaus; Pedersen, T. F.; Voß, Peter; Kind, R.; Bock, G.; Goßler, J.; Wylegala, K.; Rabbel, Wolfgang; Woelbern, I.; Budweg, Martin; Busche, H.; Korn, M.; Hock, Silke; Guterch, A.; Grad, M.; Wilde−Piórko, Monika; Zuchniak, M.; Plomerová, J.; Ansorge, Jörg; Kissling, Edi; Arlitt, R.; Waldhauser, F.; Ziegler, Peter A.; Achauer, U.; Pedersen, H.; Cotte, Nathalie; Paulssen, Hanneke; Engdahl, E. R.

doi:10.1029/99eo00001

Cited by 42 publications

(13 citation statements)

References 7 publications

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“…In central-western and northern Europe, the TOR 1996-1997 passive seismic project, which was carried out across the STZ, provided a detailed model of the upper mantle and the LAB (Gregersen et al, 1999;Shomali et al, 2006;Artlitt, 1999;Cotte et al, 2002). The results show that the average thickness of the seismic lithosphere is about 100 km in central Europe, which coincides with global tomography studies by and the studies of S receiver functions by Geissler et al (2010).…”

Section: Review Of Previous Studiessupporting

confidence: 52%

Upper mantle structure around the Trans-European Suture Zone obtained by teleseismic tomography

et al. 2015

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Abstract. The presented study aims to resolve the upper mantle structure around the Trans-European Suture Zone (TESZ), which is the major tectonic boundary in Europe. The data of 183 temporary and permanent seismic stations operated during the period of the PASsive Seismic Experiment (PASSEQ) 2006-2008 within the study area from Germany to Lithuania was used to compile the data set of manually picked 6008 top-quality arrivals of P waves from teleseismic earthquakes. We used the TELINV nonlinear teleseismic tomography algorithm to perform the inversions. As a result, we obtain a model of P wave velocity variations up to about ±3 % with respect to the IASP91 velocity model in the upper mantle around the TESZ. The higher velocities to the east of the TESZ correspond to the older East European Craton (EEC), while the lower velocities to the west of the TESZ correspond to younger western Europe. We find that the seismic lithosphere-asthenosphere boundary (LAB) is more distinct beneath the Phanerozoic part of Europe than beneath the Precambrian part. To the west of the TESZ beneath the eastern part of the Bohemian Massif, the Sudetes Mountains and the Eger Rift, the negative anomalies are observed from a depth of at least 70 km, while under the Variscides the average depth of the seismic LAB is about 100 km. We do not observe the seismic LAB beneath the EEC, but beneath Lithuania we find the thickest lithosphere of about 300 km or more. Beneath the TESZ, the asthenosphere is at a depth of 150-180 km, which is an intermediate value between that of the EEC and western Europe. The results imply that the seismic LAB in the northern part of the TESZ is in the shape of a ramp dipping to the northeasterly direction. In the southern part of the TESZ, the LAB is shallower, most probably due to younger tectonic settings. In the northern part of the TESZ we do not recognize any clear contact between Phanerozoic and Proterozoic Europe, but further to the south we may refer to a sharp and steep contact on the eastern edge of the TESZ. Moreover, beneath Lithuania at depths of 120-150 km, we observe the lower velocity area following the boundary of the proposed paleosubduction zone.

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Section: Review Of Previous Studiessupporting

confidence: 52%

Upper mantle structure around the Trans-European Suture Zone obtained by teleseismic tomography

et al. 2015

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“…Besides the tomography part the project involves receiver function studies, anisotropy studies, and geochemical and magnetotelluric studies. A similar European array deployed to study the lithosphere and asthenosphere in northern Europe by tomography is Teleseismic Tomography of the Tornquist Zone project, where 120 broadband and short‐period instruments were deployed from Germany through Denmark to Sweden [ Gregersen et al , 1999; Arlitt et al , 1999]. To analyze the structure of the mantle, information from previous refraction profiles in the region has been used to set up a three‐dimensional crustal structure model.…”

Section: Arraysmentioning

confidence: 99%

Array Seismology: Methods and Applications

Rost

Thomas

2002

Reviews of Geophysics

835

637

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Since their development in the 1960s, seismic arrays have given a new impulse to seismology. Recordings from many uniform seismometers in a well‐defined, closely spaced configuration produce high‐quality and homogeneous data sets, which can be used to study the Earth's structure in great detail. Apart from an improvement of the signal‐to‐noise ratio due to the simple summation of the individual array recordings, seismological arrays can be used in many different ways to study the fine‐scale structure of the Earth's interior. They have helped to study such different structures as the interior of volcanos, continental crust and lithosphere, global variations of seismic velocities in the mantle, the core‐mantle boundary and the structure of the inner core. For this purpose many different, specialized array techniques have been developed and applied to an increasing number of high‐quality array data sets. Most array methods use the ability of seismic arrays to measure the vector velocity of an incident wave front, i.e., slowness and back azimuth. This information can be used to distinguish between different seismic phases, separate waves from different seismic events and improve the signal‐to‐noise ratio by stacking with respect to the varying slowness of different phases. The vector velocity information of scattered or reflected phases can be used to determine the region of the Earth from whence the seismic energy comes and with what structures it interacted. Therefore seismic arrays are perfectly suited to study the small‐scale structure and variations of the material properties of the Earth. In this review we will give an introduction to various array techniques which have been developed since the 1960s. For each of these array techniques we give the basic mathematical equations and show examples of applications. The advantages and disadvantages and the appropriate applications and restrictions of the techniques will also be discussed. The main methods discussed are the beam‐forming method, which forms the basis for several other methods, different slant stacking techniques, and frequency–wave number analysis. Finally, some methods used in exploration geophysics that have been adopted for global seismology are introduced. This is followed by a description of temporary and permanent arrays installed in the past, as well as existing arrays and seismic networks. We highlight their purposes and discuss briefly the advantages and disadvantages of different array configurations.

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“…During the winter of 1996/97 an array of 120 short‐period and broad‐band seismic stations was working continuously along a c. 1000‐km‐long and 100‐km‐wide strip from Göttingen, in Germany, through Denmark, to Stockholm in Sweden. This experiment, called TOR or TOR‐1 (Gregersen et al 1999) was been established to improve knowledge of the lithospheric differences between Proterozoic and Phanerozoic Europe and delineate the transition between them. The data collected during the TOR project allow for studies of teleseismic tomography (Arlitt 1999), receiver function (Gossler et al 1999), anisotropy (Wylegalla et al 1999), scattering (Hock et al 2000) and surface waves (Cotte et al 2002).…”

Section: Introductionmentioning

confidence: 99%

Crustal structure variation from the Precambrian to Palaeozoic platforms in Europe imaged by the inversion of teleseismic receiver functions-project TOR

Wilde−Piórko

Grad

2002

Geophysical Journal International

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S U M M A R YThe TOR experiment (Teleseismic TOmography TORnquist) carried out in winter 1996/97 across the Trans-European Suture Zone (TESZ) in Germany, Denmark and Sweden has collected new data to investigate the transition zone between Precambrian and Palaeozoic Europe. In this study, seismograms of teleseismic earthquakes recorded by the broad-band TOR stations have been used to calculate the receiver functions. The time-domain inversion method has been applied to the receiver functions to compute S-wave velocities in the crust and uppermost mantle beneath each station. The results of inversion down to 60 km depth provide new, independent information about the distribution of S-wave velocity in this area. Beneath the Swedish stations on Baltica, the thickness of the crust varies from about 45 to 50 km with mostly gradually increasing S-wave velocity and no sharp discontinuities while for Danish and German stations the crust is thinner (29-38 km) with a sharp Moho discontinuity. A very distinct S-wave low velocity layer was found at depth of 8-16 km in the upper crust of Baltica, supported by the results of refraction/deep seismic sounding experiments using both P and S waves. The map of V p /V s ratio beneath the c. 1000 km long TOR 'profile' was obtained using

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Important findings expected from Europe's largest seismic array

Cited by 42 publications

References 7 publications

Upper mantle structure around the Trans-European Suture Zone obtained by teleseismic tomography

Upper mantle structure around the Trans-European Suture Zone obtained by teleseismic tomography

Array Seismology: Methods and Applications

Crustal structure variation from the Precambrian to Palaeozoic platforms in Europe imaged by the inversion of teleseismic receiver functions-project TOR

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