Search

Your search keyword '"Friederich, W."' showing total 155 results
Start Over Author "Friederich, W."
155 results on '"Friederich, W."'

3. FloodRisk – Postmining, mine water rebound, microseismicity, and ground movements

Author

Quandt, D., primary, Rische, M., additional, Niederhuber, T., additional, Allgaier, F., additional, Even, M., additional, Ukelis, O., additional, Greve, J., additional, Alber, M., additional, Busch, B., additional, Czerwonka-Schröder, D., additional, Fischer, K., additional, Friederich, W., additional, Knaak, M., additional, Müller, B., additional, Müller, L., additional, Rettenmaier, D., additional, Röckel, T., additional, Schilling, F., additional, Westerhaus, M., additional, Zorn, R., additional, and Hilgers, C., additional

Published
2023
Full Text
View/download PDF

6. Brief Mention

Author

Spiller, Robert E., Mott, Frank Luther, Friederich, W. P., Lillard, Richard G., Draper, John W., and Leary, Lewis

Published
1949

7. Imaging Seismic Wave-Fields with AlpArray and Neighboring European Networks

Author

Tesch, M., Stampa, J., Meier, T., Kissling, E., Hetényi, G., Friederich, W., Weber, M., Heit, B., Christian-Albrechts-Universität zu Kiel, Kiel, Germany, Eidgenössische Technische Hochschule Zürich, Zurich, Switzerland, Université de Lausanne, Lausanne, Switzerland, Ruhr-Universität Bochum, Bochum, Germany, Universität Potsdam, Potsdam, Germany, and Deutsches GeoForschungsZentrum Potsdam, Potsdam, Germany

Subjects
Wavefront, Tomographic reconstruction, Wave-fields, Alps, Plane wave, Sampling (statistics), ddc:551.22, Swath-D, Seismic wave, Physics::Geophysics, Wavelength, Surface wave, Seismology, Animations, AlpArray, Moment (physics), Broadband, General Earth and Planetary Sciences, Point (geometry), Seismogram, Geology
Abstract

The AlpArray experiment and the deployment of Swath-D together with the dense permanent network in Italy allow for detailed imaging of the spatio-temporal imaging complexity of seismic wave-fields within the greater Alpine region. The distance of any point within the area to the nearest station is less than 30 km, resulting in an average inter-station distance of about 45 km. With a much denser deployment in a smaller region of the Alps (320 km in length and 140 km wide), the Swath-D network possesses an average inter-station distance of about 15 km. We show that seismogram sections with a spatial sampling of less than 5 km can be obtained using recordings of these regional arrays for just a single event. Multiply reflected body waves can be observed for up to 2 h after source time. In addition, we provide and describe animations of long-period seismic wave-fields using recordings of about 1300-1600 broadband stations for six representative earthquakes. These illustrate the considerable spatio-temporal variability of the wave-field's properties at a high lateral resolution. Within denser station distributions like those provided by Swath-D, even shorter period body and surface wave features can be recovered. The decrease of the horizontal wavelength from P to S to surface waves, deviations from spherically symmetric wavefronts, and the capability to detect multi-orbit arrivals are demonstrated qualitatively by the presented wave-field animations, which are a valuable tool for educational, quality control, and research purposes. We note that the information content of the acquired datasets can only be adequately explored by application of appropriate quantitative methods accounting for the considerable complexity of the seismic wave-fields as revealed by the now available station configuration., International Journal of Earth Sciences, 111 (1), ISSN:1437-3254, ISSN:1437-3262

Published
2020

8. Coda-Q in the 2.5-20 s period band from seismic noise : application to the greater Alpine area

Author

Soergel, D., Pedersen, H. A., Stehly, L., Margerin, L., Paul, A., Hetenyi, G., Abreu, R., Allegretti, I., Apoloner, M. T., Aubert, C., De Berc, M. B., Bokelmann, G., Brunel, D., Capello, M., Carman, M., Cavaliere, A., Cheze, J., Chiarabba, C., Clinton, J., Cougoulat, G., Crawford, W., Cristiano, L., Czifra, T., D'Alema, E., Danesi, S., Daniel, R., Dasovic, I., Deschamps, A., Dessa, J. X., Doubre, C., Egdorf, S., Fiket, T., Fischer, K., Friederich, W., Fuchs, F., Funke, S., Giardini, D., Govoni, A., Graczer, Z., Groschl, G., Heimers, S., Heit, B., Herak, D., Herak, M., Huber, J., Jaric, D., Jedlicka, P., Jia, Y., Jund, H., Kissling, E., Klingen, S., Klotz, B., Kolinsky, P., Korn, M., Kotek, J., Kuhne, L., Kuk, K., Loos, J., Malengros, D., Margheriti, L., Maron, C., Martin, X., Massa, M., Mazzarini, F., Meier, T., Metral, L., Molinari, I., Moretti, M., Munzarova, H., Nardi, A., Pahor, J., Pequegnat, C., Pesaresi, D., Piccinini, D., Piromallo, C., Plenefisch, T., Plomerova, J., Pondrelli, S., Prevolnik, S., Racine, R., Régnier, Marc, Reiss, M., Ritter, J., Rumpker, G., Salimbeni, S., Schulte-Kortnack, D., Scherer, W., Schippkus, S., Sipka, V., Spallarossa, D., Spieker, K., Stipcevic, J., Strollo, A., Sule, B., Szanyi, G., Szucs, E., Thomas, C., Tilmann, F., Ueding, S., Vallocchia, M., Vecsey, L., Voigt, R., Wassermann, J., Weber, Z., Weidle, C., Wesztergom, V., Weyland, G., Wiemer, S., Wolyniec, D., Zieke, T., Zivvic, M., and AlpArray Working Group

Subjects
Europe, surface waves and free oscillations, Coda waves, seismic attenuation, seismic noise, wave scattering and diffraction
Abstract

Coda-Q is used to estimate the attenuation and scattering properties of the Earth. So far focus has been on earthquake data at frequencies above 1 Hz, as the high noise level in the first and second microseismic peak, and possibly lower scattering coefficient, hinder stable measurements at lower frequencies. In this work, we measure and map coda-Q in the period bands 2.5-5 s, 5-10 s and 10-20 s in the greater Alpine region using noise cross-correlations between station pairs, based on data from permanent seismic stations and from the temporary AlpArray experiment. The observed coda-Q for short interstation distances is independent of azimuth so there is no indication of influence of the directivity of the incoming noise field on our measurements. In the 2.5-5 s and 5-10 s period bands, our measurements are self-consistent, and we observe stable geographic patterns of low and high coda-Q in the period bands 2.5-5 s and 5-10 s. In the period band 10-20 s, the dispersion of our measurements increases and geographic patterns become speculative. The coda-Q maps show that major features are observed with high resolution, with a very good geographical resolution of for example low coda-Q in the Po Plain. There is a sharp contrast between the Po Plain and the Alps and Apennines where coda-Q is high, with the exception a small area in the Swiss Alps which may be contaminated by the low coda-Q of the Po Plain. The coda of the correlations is too short to make independent measurements at different times within the coda, so we cannot distinguish between intrinsic and scattering Q. Measurements on more severely selected data sets and longer time-series result in identical geographical patterns but lower numerical values. Therefore, high coda-Q values may be overestimated, but the geographic distribution between high and low coda-Q areas is respected. Our results demonstrate that noise correlations are a promising tool for extending coda-Q measurements to frequencies lower than those analysed with earthquake data.

Published
2020

12. Receiver function images of the Hellenic subduction zone and comparison to microseismicity

Author

Sodoudi, F., Brüstle, A., Meier, T., Kind, R., Friederich, W., and EGELADOS working group

Subjects
Mantle wedge, Subduction, Stratigraphy, Continental crust, lcsh:QE1-996.5, Paleontology, Soil Science, Geology, Mantle (geology), lcsh:Geology, African Plate, Geophysics, lcsh:Stratigraphy, Geochemistry and Petrology, Oceanic crust, Lithosphere, Eclogitization, Seismology, lcsh:QE640-699, Earth-Surface Processes
Abstract

New combined P receiver functions and seismicity data obtained from the EGELADOS network employing 65 seismological stations within the Aegean constrained new information on the geometry of the Hellenic subduction zone. The dense network and large data set enabled us to estimate the Moho depth of the continental Aegean plate across the whole area. Presence of a negative contrast at the Moho boundary indicating the serpentinized mantle wedge above the subducting African plate was seen along the entire forearc. Furthermore, low seismicity was observed within the serpentinized mantle wedge. We found a relatively thick continental crust (30–43 km) with a maximum thickness of about 48 km beneath the Peloponnese Peninsula, whereas a thinner crust of about 27–30 km was observed beneath western Turkey. The crust of the overriding plate is thinning beneath the southern and central Aegean and reaches 23–27 km. Unusual low Vp / Vs ratios were estimated beneath the central Aegean, which most likely represent indications on the pronounced felsic character of the extended continental Aegean crust. Moreover, P receiver functions imaged the subducted African Moho as a strong converted phase down to a depth of about 100 km. However, the converted Moho phase appears to be weak for the deeper parts of the African plate suggesting nearly complete phase transitions of crustal material into denser phases. We show the subducting African crust along eight profiles covering the whole southern and central Aegean. Seismicity of the western Hellenic subduction zone was taken from the relocated EHB-ISC catalogue, whereas for the eastern Hellenic subduction zone, we used the catalogues of manually picked hypocentre locations of temporary networks within the Aegean. Accurate hypocentre locations reveal a significant change in the dip angle of the Wadati–Benioff zone (WBZ) from west (~ 25°) to the eastern part (~ 35°) of the Hellenic subduction zone. Furthermore, a zone of high deformation can be characterized by a vertical offset of about 40 km of the WBZ beneath the eastern Cretan Sea. This deformation zone may separate a shallower N-ward dipping slab in the west from a steeper NW-ward dipping slab in the east. In contrast to hypocentre locations, we found very weak evidence for the presence of the slab at larger depths in the P receiver functions, which may result from the strong appearance of the Moho multiples as well as eclogitization of the oceanic crust. The presence of the top of a strong low-velocity zone at about 60 km depth in the central Aegean may be related to the asthenosphere below the Aegean continental lithosphere and above the subducting slab. Thus, the Aegean mantle lithosphere seems to be 30–40 km thick, which means that its thickness increased again since the removal of the mantle lithosphere about 15 to 35 Ma ago.

Published
2018

14. Structure of cyclin G-associated kinase (GAK) trapped in different conformations using nanobodies

Author

Apirat Chaikuad, Tracy Keates, Cécile Vincke, Melanie Kaufholz, Michael Zenn, Zimmermann Bastian, Carlos Gutiérrez, Rong-Guang Zhang, Catherine Hatzos-Skintges, Andrzej Joachimiak, Serge Muyldermans, Herberg, Friederich W., Knapp, S., Muller, S., and Cellular and Molecular Immunology

Subjects
SeMet, selenomethionine, Camelus, kinase inhibitor, Protein Conformation, MPSK1, myristoylated and palmitoylated serine/threonine kinase 1, DARPin, designed ankyrin-repeat protein, SPR, surface plasmon resonance, Protein Serine-Threonine Kinases, Nb, nanobody, CDR, complementarity-determining region, Catalytic Domain, Animals, Humans, GAK, cyclin G-associated kinase, protein structure, ASCH, activation segment C-terminal helix, HA, haemagglutinin, AUC, analytical ultracentrifugation, TCEP, tris-(2-carboxyethyl)phosphine, cyclin G-associated kinase, NAK, numb-associated kinase, Intracellular Signaling Peptides and Proteins, drug side effect, activation loop, TEV, Tobacco etch virus, Single-Domain Antibodies, EGFR, epidermal growth factor receptor, GAK kinase, Enzyme Activation, nanobody, RU, resonance unit, Protein Multimerization, Apoproteins, Crystallization, Research Article
Abstract

GAK (cyclin G-associated kinase) is a key regulator of clathrin-coated vesicle trafficking and plays a central role during development. Additionally, due to the unusually high plasticity of its catalytic domain, it is a frequent ‘off-target’ of clinical kinase inhibitors associated with respiratory side effects of these drugs. In the present paper, we determined the crystal structure of the GAK catalytic domain alone and in complex with specific single-chain antibodies (nanobodies). GAK is constitutively active and weakly associates in solution. The GAK apo structure revealed a dimeric inactive state of the catalytic domain mediated by an unusual activation segment interaction. Co-crystallization with the nanobody NbGAK_4 trapped GAK in a dimeric arrangement similar to the one observed in the apo structure, whereas NbGAK_1 captured the activation segment of monomeric GAK in a well-ordered conformation, representing features of the active kinase. The presented structural and biochemical data provide insight into the domain plasticity of GAK and demonstrate the utility of nanobodies to gain insight into conformational changes of dynamic molecules. In addition, we present structural data on the binding mode of ATP mimetic inhibitors and enzyme kinetic data, which will support rational inhibitor design of inhibitors to reduce the off-target effect on GAK., Cyclin G-associated kinase (GAK) is a regulator of clathrin-coated vesicle trafficking. The determined crystal structures of GAK in complex with specific single chain antibodies (nanobodies) revealed the domain plasticity of this kinase and unusual activation segment architecture.

Published
2014
Full Text
View/download PDF

16. Goethe

Author

Friederich, W. P.

Published
1949

21. A nodal discontinuous Galerkin approach to 3-D viscoelastic wave propagation in complex geological media.

Author

Lambrecht, L., Lamert, A., Friederich, W., Möller, T., and Boxberg, M. S.

Subjects
SEISMOLOGY, THEORY of wave motion, VISCOELASTICITY, GALERKIN methods, SEISMIC waves
Abstract

A nodal discontinuous Galerkin (NDG) approach is developed and implemented for the computation of viscoelasticwavefields in complex geological media. TheNDGapproach combines unstructured tetrahedral meshes with an element-wise, high-order spatial interpolation of the wavefield based on Lagrange polynomials. Numerical fluxes are computed from an exact solution of the heterogeneous Riemann problem. Our implementation offers capabilities for modelling viscoelastic wave propagation in 1-D, 2-D and 3-D settings of very different spatial scale with little logistical overhead. It allows the import of external tetrahedral meshes provided by independent meshing software and can be run in a parallel computing environment. Computation of adjoint wavefields and an interface for the computation of waveform sensitivity kernels are offered. The method is validated in 2-D and 3-D by comparison to analytical solutions and results from a spectral element method. The capabilities of the NDG method are demonstrated through a 3-D example case taken from tunnel seismics which considers high-frequency elastic wave propagation around a curved underground tunnel cutting through inclined and faulted sedimentary strata. The NDG method was coded into the open-source software package NEXD and is available from GitHub. [ABSTRACT FROM AUTHOR]

Published
2018
Full Text
View/download PDF

22. Real time monitoring of moment magnitude by waveform inversion

Author

Lee, J., Friederich, W., and Meier, T.

Subjects
Physics::Geophysics
Abstract

An instantaneous measure of the moment magnitude (Mw) of an ongoing earthquake is estimated from the moment rate function (MRF) determined in real-time from available seismic data using waveform inversion. Integration of the MRF gives the moment function from which an instantaneousMw is derived. By repeating the inversion procedure at regular intervals while seismic data are coming in we can monitor the evolution of seismic moment and Mw with time. The final size and duration of a strong earthquake can be obtained within 12 to 15 minutes after the origin time. We show examples of Mw monitoring for three large earthquakes at regional distances. The estimated Mw is only weakly sensitive to changes in the assumed source parameters. Depending on the availability of seismic stations close to the epicenter, a rapid estimation of the Mw as a prerequisite for the assessment of earthquake damage potential appears to be feasible.

Published
2012

23. TOAST (TOolbox for Applied Seismic Tomography)

Author

Barsch, R., Bohlen, T., Dunkl, S., Fischer, L., Forbriger, T., Friederich, W., Giese, R., Igel, H., Krompholz, R., Lüth, S., Meier, T., Mosca, I., Rehor, L., Schäfer, M., Schuck, A., Sigloch, K., and Schumacher, F.

Abstract

The time has come to exploit the full richness of broadband, three-component waveforms. The inversion of full seismograms leads to a tremendous improvement in imaging resolution due to the ability to map structures that are smaller than the seismic wavelength. In addition, it provides important constraints on density and attenuation. State-of-the-art software for full waveform tomography is available in scientific environments but is not yet accessible to the practitioner. The Toolbox for Applied Seismic Tomography (TOAST) will open a new window to seismic inversion. Due to advances in available computational resources and recent developments in high performance and parallelized computing, 3D inversion of full seismograms is within reach. By combining tested code collections for waveform modelling and the solution of large inverse problems, complemented by experience in the management of large software projects and by sound expertise in the inversion of elastic waves from the centimeter to the kilometer scale, the cooperation of the TOAST project partners will provide a unique knowledge base for implementing flexible and efficient tools for full waveform tomography and to transfer the knowledge to industrial practice. The TOAST project pursues the concept of modularization. It will provide modules that interact through standardized interfaces and thereby can be re-combined in application-specific and efficient ways. The Toolbox for Applied Seismic Tomography will prove its worth through application to surveys from commercial practice. Existing data from seismic experiments at different scales (e.g., monitoring of embankments, CO2 sequestration studies) and newly aquired shallow seismic and ultrasonic data will serve as case studies to validate the functionality of the toolbox.

Published
2011
Full Text
View/download PDF

24. Dynamische Erde - Zukunftsaufgaben der Geowissenschaften : Strategieschrift

Author

Andruleit, H., Bach, W., Balzer, D., Bau, M., Becker, H., Bendix, J., Bens, O., Bill, R., Bismayer, U., von Blanckenburg, F., Blotevogel, H., Boetius, A., Bork, H., Bosbach, D., Bräuer, V., Brückner, H., Buchholz, P., Bunge, P., Cermak, J., Chakraborty, S., Christensen, U., Clauser, C., Claußen, M., Cubasch, U., Delisle, G., Deutsch, A., Diepenbroek, M., Dikau, R., Dingwell, D., Dott, W., Dresen, G., Dürr, S., Elsner, H., Emmermann, R., Erbacher, J., Flurly, J., Franke, W., Franz, G., Freiwald, A., Friederich, W., Friedrich, A., Frost, D., Gaupp, R., Gebhardt, H., Gerling, P., Gestermann, N., Gleixner, G., Grathwohl, P., Günther, A., Handy, M., Hartmann, J., Heinrich, W., Hemmer, I., Hennings, V., Hezel, D., Hinderer, M., Horsfield, B., Huch, M., Hüser, K., Hüttl, R., Isenbeck-Schröter, M., Keppler, H., Kiessling, W., Kind, R., Kolditz, O., Kothe, E., Kraas, F., Kudrass, H., Kuhn, D., Kühn, M., Kümpel, H., Langenhorst, F., Leiss, B., Leythäuser, D., Littke, R., Maronde, D., MacCammon, C., Megerle, H., Mezger, K., Mosbrugger, V., Mulch, A., Münker, C., Ochmann, N., Oncken, O., Otto, K., Palme, H., Peckmann, J., Pollock, K., di Primio, R., Radtke, U., Ranke, U., Reichert, C., Röhling, S., Rust, J., Samuel, H., Scheck-Wenderoth, M., Scherbaum, F., Schmidt, U., Schmidt-Thome, M., Schulz, M., Schütt, B., Schwalb, A., Schwarz-Schampera, U., Sester, M., Spohn, T., Steinbach, V., Steininger, F., Steinle-Neumann, G., Stöckhert, B., Stöffler, D., Strecker, M., Thiede, J., Tischner, T., Trumbull, R., Ulbrich, U., Vasters, J., Vereecken, H., Wagner, M., Weber, M., Wefer, G., Wellmer, F., Welte, D., Wenzel, F., Westphal, H., Wiesmüller, G., Wippermann, T., Woith, H., Wörner, G., Zschau, J., Wefer, G., and WB Scientific Drilling, Scientific Infrastructure and Plattforms, GFZ Publication Database, Deutsches GeoForschungsZentrum

Subjects
550 - Earth sciences
Published
2010

26. Long-term outcome following hematopoietic stem cell transplantation in Wiskott-Aldrich syndrome: collaborative study of the European Society for Immunodeficiencies and the European Group for Blood and Marrow Transplantation

Author

Ozsahin, H, CAVAZZANA CALVO, M, Notarangelo, Luigi Daniele, Schulz, A, Thrasher, Aj, Mazzolari, Evelina, Slatter, Ma, LE DEIST, F, Blanche, S, Veys, P, Fasth, A, Bredius, R, Sedlacek, P, Wulfraat, N, Ortega, J, Heilmann, C, O'Meara, A, Wachowiak, J, Kalwak, K, MATTHES MARTIN, S, Gungor, T, Ikinciogullari, A, Landais, P, Cant, Aj, Friederich, W, and Fisher, A.

Published
2007

28. Complex lithospheric structure under the central Baltic Shield from surface wave tomography

Author

Bruneton, M., Pedersen, Helle A., Farra, Véronique, Arndt, Nicholas, Vacher, P., Achauer, U., Alinaghi, A., Ansorge, J., Bock, G., Friederich, W., Grad, M., Guterch, A., Heikkinen, P., Hjelt, S., Hyvonen, T., Ikonen, J.P., Kissling, E., Komminaho, K., Korja, A., Kozlovskaya, E., Nevsky, M., Paulssen, H., Pavlenkova, N., Plomerova, J., Raita, T., Riznichenko, O.Y., Roberts, R., Sandoval, S., Sanina, I., Sharov, N., Shomali, Z., Tiikkainen, J., Wielandt, E., Wilegalla, K., Yliniemi, J., Yurov, Y., Laboratoire de Géophysique Interne et Tectonophysique (LGIT), Institut des Sciences de la Terre [2011-2015] (ISTerre [2011-2015]), Université Joseph Fourier - Grenoble 1 (UJF)-Institut Français des Sciences et Technologies des Transports, de l'Aménagement et des Réseaux (IFSTTAR)-Institut national des sciences de l'Univers (INSU - CNRS)-Institut de recherche pour le développement [IRD] : UR219-PRES Université de Grenoble-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut Français des Sciences et Technologies des Transports, de l'Aménagement et des Réseaux (IFSTTAR)-Institut national des sciences de l'Univers (INSU - CNRS)-Institut de recherche pour le développement [IRD] : UR219-PRES Université de Grenoble-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Laboratoire Central des Ponts et Chaussées (LCPC)-Observatoire des Sciences de l'Univers de Grenoble [1985-2015] (OSUG [1985-2015]), Centre National de la Recherche Scientifique (CNRS)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut polytechnique de Grenoble - Grenoble Institute of Technology [2007-2019] (Grenoble INP [2007-2019])-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Institut polytechnique de Grenoble - Grenoble Institute of Technology [2007-2019] (Grenoble INP [2007-2019])-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA), Institut de Physique du Globe de Paris (IPGP), Université Pierre et Marie Curie - Paris 6 (UPMC)-Institut national des sciences de l'Univers (INSU - CNRS)-IPG PARIS-Université Paris Diderot - Paris 7 (UPD7)-Université de La Réunion (UR)-Centre National de la Recherche Scientifique (CNRS), Laboratoire de Géodynamique des Chaines Alpines (LGCA), Observatoire des Sciences de l'Univers de Grenoble [1985-2015] (OSUG [1985-2015]), Centre National de la Recherche Scientifique (CNRS)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut polytechnique de Grenoble - Grenoble Institute of Technology [2007-2019] (Grenoble INP [2007-2019])-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut polytechnique de Grenoble - Grenoble Institute of Technology [2007-2019] (Grenoble INP [2007-2019])-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Institut national des sciences de l'Univers (INSU - CNRS)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Institut des Sciences de la Terre [2011-2015] (ISTerre [2011-2015]), Université Joseph Fourier - Grenoble 1 (UJF)-Institut Français des Sciences et Technologies des Transports, de l'Aménagement et des Réseaux (IFSTTAR)-Institut national des sciences de l'Univers (INSU - CNRS)-Institut de recherche pour le développement [IRD] : UR219-PRES Université de Grenoble-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Institut Français des Sciences et Technologies des Transports, de l'Aménagement et des Réseaux (IFSTTAR)-Institut de recherche pour le développement [IRD] : UR219-PRES Université de Grenoble-Centre National de la Recherche Scientifique (CNRS), Laboratoire de Planétologie et Géodynamique [UMR 6112] (LPG), Centre National de la Recherche Scientifique (CNRS)-Institut national des sciences de l'Univers (INSU - CNRS)-Université de Nantes - Faculté des Sciences et des Techniques, Université de Nantes (UN)-Université de Nantes (UN)-Université d'Angers (UA), Ecole et Observatoire des sciences de la terre (EOST), Centre National de la Recherche Scientifique (CNRS)-Université Louis Pasteur - Strasbourg I-Institut national des sciences de l'Univers (INSU - CNRS), Observatoire des Sciences de l'Univers de Grenoble (OSUG), Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Institut polytechnique de Grenoble - Grenoble Institute of Technology (Grenoble INP)-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Université Grenoble Alpes (UGA)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Institut polytechnique de Grenoble - Grenoble Institute of Technology (Grenoble INP)-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Université Grenoble Alpes (UGA)-Laboratoire Central des Ponts et Chaussées (LCPC)-Institut des Sciences de la Terre (ISTerre), Université Grenoble Alpes (UGA)-Centre National de la Recherche Scientifique (CNRS)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-PRES Université de Grenoble-Institut de recherche pour le développement [IRD] : UR219-Institut national des sciences de l'Univers (INSU - CNRS)-Institut Français des Sciences et Technologies des Transports, de l'Aménagement et des Réseaux (IFSTTAR)-Université Joseph Fourier - Grenoble 1 (UJF)-Centre National de la Recherche Scientifique (CNRS)-PRES Université de Grenoble-Institut de recherche pour le développement [IRD] : UR219-Institut Français des Sciences et Technologies des Transports, de l'Aménagement et des Réseaux (IFSTTAR), Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Institut polytechnique de Grenoble - Grenoble Institute of Technology (Grenoble INP)-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Université Grenoble Alpes (UGA)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Institut polytechnique de Grenoble - Grenoble Institute of Technology (Grenoble INP)-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)-Université Grenoble Alpes (UGA)-Institut des Sciences de la Terre (ISTerre), Laboratoire de Planétologie et Géodynamique UMR6112 (LPG), Laboratoire Central des Ponts et Chaussées (LCPC)-Observatoire des Sciences de l'Univers de Grenoble (OSUG), Université Joseph Fourier - Grenoble 1 (UJF)-Institut polytechnique de Grenoble - Grenoble Institute of Technology (Grenoble INP )-Institut national des sciences de l'Univers (INSU - CNRS)-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Université Joseph Fourier - Grenoble 1 (UJF)-Institut polytechnique de Grenoble - Grenoble Institute of Technology (Grenoble INP )-Institut national des sciences de l'Univers (INSU - CNRS)-Institut national de recherche en sciences et technologies pour l'environnement et l'agriculture (IRSTEA)-Université Savoie Mont Blanc (USMB [Université de Savoie] [Université de Chambéry])-Centre National de la Recherche Scientifique (CNRS)-Centre National de la Recherche Scientifique (CNRS), Université d'Angers (UA)-Université de Nantes - UFR des Sciences et des Techniques (UN UFR ST), Université de Nantes (UN)-Université de Nantes (UN)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS), Institut national des sciences de l'Univers (INSU - CNRS)-Université Louis Pasteur - Strasbourg I-Centre National de la Recherche Scientifique (CNRS), and 2.4 Seismology, 2.0 Physics of the Earth, Departments, GFZ Publication Database, Deutsches GeoForschungsZentrum

Subjects
[SDU.STU.GP]Sciences of the Universe [physics]/Earth Sciences/Geophysics [physics.geo-ph], [SDE.MCG]Environmental Sciences/Global Changes, 550 - Earth sciences, [PHYS.PHYS.PHYS-GEO-PH]Physics [physics]/Physics [physics]/Geophysics [physics.geo-ph], [SDE.MCG.CPE]Environmental Sciences/Global Changes/domain_sde.mcg.cpe, ComputingMilieux_MISCELLANEOUS, Physics::Geophysics
Abstract

International audience; [1] Regional seismic tomography provides valuable information on the structure of shields, thereby gaining insight to the formation and stabilization of old continents. Fennoscandia (known as the Baltic Shield for its exposed part) is a composite shield for which the last recorded tectonic event is the intrusion of the Rapakivi granitoids around 1.6 Ga. A seismic experiment carried out as part of the European project Svecofennian-Karelia-Lapland-Kola (SVEKALAPKO) was designed to study the upper mantle of the Finnish part of the Baltic Shield, especially the boundary between Archean and Proterozoic domains. We invert the fundamental mode Rayleigh waves to obtain a three-dimensional shear wave velocity model using a ray-based method accounting for the curvature of wave fronts. The experiment geometry allows an evaluation of lateral variations in velocities down to 150 km depth. The obtained model exhibits variations of up to ±3% in S wave velocities. As the thermal variations beneath Finland are very small, these lateral variations must be caused by different rock compositions. The lithospheres beneath the Archean and Proterozoic domains are not noticeably different in the S wave velocity maps. A classification of the velocity profiles with depth yields four main families and five intermediate regions that can be correlated with surface features. The comparison of these profiles with composition-based shear wave velocities implies both lateral and vertical variations of the mineralogy. INDEX TERMS: 7218 Seismology: Lithosphere and upper mantle; 7255 Seismology: Surface waves and free oscillations; 8180 Tectonophysics: Tomography; 9619 Information Related to Geologic Time: Precambrian; 1025 Geochemistry: Composition of the mantle; KEYWORDS: lithosphere, surface wave, Baltic Shield Citation: Bruneton, M., et al. (2004), Complex lithospheric structure under the central Baltic Shield from surface wave tomography

Published
2004

29. Layered lithospheric mantle in the central Baltic shield from surface wave and xenolith analysis

Author

Bruneton, M., H.A., Pedersen, Vacher, P., I.T., Kukkonen, N.T., Arndt, Funke, S., Friederich, W., Farra, V., Group, Svekalapko, Laboratoire de Planétologie et Géodynamique [UMR 6112] (LPG), Université d'Angers (UA)-Université de Nantes - UFR des Sciences et des Techniques (UN UFR ST), and Université de Nantes (UN)-Université de Nantes (UN)-Institut national des sciences de l'Univers (INSU - CNRS)-Centre National de la Recherche Scientifique (CNRS)

Subjects
ComputingMilieux_MISCELLANEOUS, Structures Internes et Evolution comparée des planètes
Abstract

International audience

Published
2004

37. A flexible, extendable, modular and computationally efficient approach to scattering-integral-based seismic full waveform inversion.

Author

Schumacher, F., Friederich, W., and Lamara, S.

Subjects
*SEISMIC waves, *INVERSION (Geophysics), *THEORY of wave motion, *SEISMIC tomography, *NUMERICAL analysis, *ITERATIVE methods (Mathematics), *PROBLEM solving
Abstract

We present a new conceptual approach to scattering-integral-based seismic full waveform inversion (FWI) that allows a flexible, extendable, modular and both computationally and storage-efficient numerical implementation. To achieve maximum modularity and extendability, interactions between the three fundamental steps carried out sequentially in each iteration of the inversion procedure, namely, solving the forward problem, computingwaveformsensitivity kernels and deriving a model update, are kept at an absolute minimum and are implemented by dedicated interfaces. To realize storage efficiency and maximum flexibility, the spatial discretization of the inverted earth model is allowed to be completely independent of the spatial discretization employed by the forward solver. For computational efficiency reasons, the inversion is done in the frequency domain. The benefits of our approach are as follows: (1) Each of the three stages of an iteration is realized by a stand-alone software program. In this way, we avoid the monolithic, unflexible and hard-to-modify codes that have often been written for solving inverse problems. (2) The solution of the forward problem, required for kernel computation, can be obtained by any wave propagation modelling code giving users maximum flexibility in choosing the forward modelling method. Both time-domain and frequency-domain approaches can be used. (3) Forward solvers typically demand spatial discretizations that are significantly denser than actually desired for the inverted model. Exploiting this fact by pre-integrating the kernels allows a dramatic reduction of disk space and makes kernel storage feasible. No assumptions are made on the spatial discretization scheme employed by the forward solver. (4) In addition, working in the frequency domain effectively reduces the amount of data, the number of kernels to be computed and the number of equations to be solved. (5) Updating the model by solving a large equation system can be done using different mathematical approaches. Since kernels are stored on disk, it can be repeated many times for different regularization parameters without need to solve the forward problem, making the approach accessible to Occam's method. Changes of choice of misfit functional, weighting of data and selection of data subsets are still possible at this stage. We have coded our approach to FWI into a program package called ASKI (Analysis of Sensitivity and Kernel Inversion) which can be applied to inverse problems at various spatial scales in both Cartesian and spherical geometries. It is written in modern FORTRAN language using object-oriented concepts that reflect the modular structure of the inversion procedure. We validate our FWI method by a small-scale synthetic study and present first results of its application to high-quality seismological data acquired in the southern Aegean. [ABSTRACT FROM AUTHOR]

Published
2016
Full Text
View/download PDF

43. Receiver function images of the Hellenic subduction zone and comparison to microseismicity.

Author

Sodoudi, F., Brüstle, A., Meier, T., Kind, R., and Friederich, W.

Subjects
SUBDUCTION zones, SEISMOLOGICAL stations, BENIOFF zones, LITHOSPHERE, EARTH'S mantle, CRUST of the earth
Abstract

New combined P receiver functions and seismicity data obtained from the EGELADOS network employing 65 seismological stations within the Aegean constrained new information on the geometry of the Hellenic subduction zone. The dense network and large data set enabled us to estimate the Moho depth of the continental Aegean plate across the whole area. Presence of a negative contrast at the Moho boundary indicating the serpentinized mantle wedge above the subducting African plate was seen along the entire forearc. Furthermore, low seismicity was observed within the serpentinized mantle wedge. We found a relatively thick continental crust (30-43 km) with a maximum thickness of about 48 km beneath the Peloponnese Peninsula, whereas a thinner crust of about 27-30 km was observed beneath western Turkey. The crust of the overriding plate is thinning beneath the southern and central Aegean and reaches 23-27 km. Unusual low Vp / Vs ratios were estimated beneath the central Aegean, which most likely represent indications on the pronounced felsic character of the extended continental Aegean crust. Moreover, P receiver functions imaged the subducted African Moho as a strong converted phase down to a depth of about 100 km. However, the converted Moho phase appears to be weak for the deeper parts of the African plate suggesting nearly complete phase transitions of crustal material into denser phases. We show the subducting African crust along eight profiles covering the whole southern and central Aegean. Seismicity of the western Hellenic subduction zone was taken from the relocated EHB-ISC catalogue, whereas for the eastern Hellenic subduction zone, we used the catalogues of manually picked hypocentre locations of temporary networks within the Aegean. Accurate hypocentre locations reveal a significant change in the dip angle of the Wadati-Benioff zone (WBZ) from west (~25°) to the eastern part (~35°) of the Hellenic subduction zone. Furthermore, a zone of high deformation can be characterized by a vertical offset of about 40 km of the WBZ beneath the eastern Cretan Sea. This deformation zone may separate a shallower N-ward dipping slab in the west from a steeper NW-ward dipping slab in the east. In contrast to hypocentre locations, we found very weak evidence for the presence of the slab at larger depths in the P receiver functions, which may result from the strong appearance of the Moho multiples as well as eclogitization of the oceanic crust. The presence of the top of a strong low-velocity zone at about 60 km depth in the central Aegean may be related to the asthenosphere below the Aegean continental lithosphere and above the subducting slab. Thus, the Aegean mantle lithosphere seems to be 30-40 km thick, which means that its thickness increased again since the removal of the mantle lithosphere about 15 to 35 Ma ago. [ABSTRACT FROM AUTHOR]

Published
2015
Full Text
View/download PDF

46. Complex lithospheric structure under the central Baltic Shield from surface wave tomography

Author

Bruneton, Marianne, primary, Pedersen, Helle A., additional, Farra, Véronique, additional, Arndt, Nicholas T., additional, Vacher, Pierre, additional, Achauer, U., additional, Alinaghi, A., additional, Ansorge, J., additional, Bock, G., additional, Friederich, W., additional, Grad, M., additional, Guterch, A., additional, Heikkinen, P., additional, Hjelt, S.‐E., additional, Hyvönen, T. L., additional, Ikonen, J.‐P., additional, Kissling, E., additional, Komminaho, K., additional, Korja, A., additional, Kozlovskaya, E., additional, Nevsky, M. V., additional, Paulssen, H., additional, Pavlenkova, N. I., additional, Plomerová, J., additional, Raita, T., additional, Riznichenko, O. Y., additional, Roberts, R. G., additional, Sandoval, S., additional, Sanina, I. A., additional, Sharov, N. V., additional, Shomali, Z. H., additional, Tiikkainen, J., additional, Wielandt, E., additional, Wilegalla, K., additional, Yliniemi, J., additional, and Yurov, Y. G., additional

Published
2004
Full Text
View/download PDF

49. Seismic probing of Fennoscandian lithosphere

Author

Bock, G., primary, Achauer, U., additional, Alinaghi, A., additional, Ansorge, J., additional, Bruneton, M., additional, Friederich, W., additional, Grad, M., additional, Guterch, A., additional, Hjelt, S. -E., additional, Hyv"nen, T., additional, Ikonen, J.-P., additional, Kissling, E., additional, Komminaho, K., additional, Korja, A., additional, Heikkinen, P., additional, Kozlovskaya, E., additional, Nevsky, M. V., additional, Pavlenkova, N., additional, Pedersen, H., additional, Plomerov, J., additional, Raita, T., additional, Riznichenko, O., additional, Roberts, R. G., additional, Sandoval, S., additional, Sanina, I. A., additional, Sharov, N., additional, Tiikkainen, J., additional, Volosov, S. G., additional, Wielandt, E., additional, Wylegalla, K., additional, Yliniemi, J., additional, and Yurov, Y., additional

Published
2001
Full Text
View/download PDF

Catalog

Books, media, physical & digital resources
See catalog results