2. Mineralogy – Petrology – Geochemistry - SWISS GEOSCIENCE ...

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4 Plenary Session 0. Plenary Session 1 Halliday, Alex N.: The origin of the Earth and its volatiles 2 Kump, Lee R.: Emergence of an Aerobic Biosphere during the Archean-Proterozoic Transition 3 MacLeod, Norman: ‘Mass Extinctions’ in the Geological Record: Causes and Consequences 4 Boetius, Antje: Geosphere-Biosphere Interactions: Methane-based life at the ocean floor 5 Imboden, Dieter: Will research save planet Earth? Swiss Geoscience Meeting 2011 Platform Geosciences, Swiss Academy of Science, SCNAT
1 The origin of the Earth and its volatiles Alex N Halliday Oxford University The origin of Earth is well explained by oligarchic accretion of planetesimals and planetary embryos over tens of millions of years. The last major event is thought to have been the Moon forming Giant Impact which added about 10% of the planet’s mass. Tungsten isotopic evidence demonstrates that the Earth’s core grew during accretion. Comparisons with meteorite data for other bodies suggest that it may also have grown in relative proportion over time. The depletion of slightly siderophile elements such as vanadium is consistent with a primitive mantle that was more reduced during the earlier stages of accretion. This is confirmed by isotopic evidence that the core had sequestered a significant amount of silicon before the Giant Impact. Despite these advances in our understanding of the past 20 years there are significant issues that have not been resolved. The timing of the Giant Impact is still argued about with recently proposed ages ranging from 30 to 200 million years after the start of the solar system, extending to the ages of the oldest detrital zircon grains yet discovered on Earth. Similarly there still is no consensus about how water and other highly volatile elements were added to Earth. The final (70%) of the hydrogen (water) budget is earlier, which is hard to reconcile with the hot dry early Earth models advocated by some. 2 Emergence of an Aerobic Biosphere during the Archean-Proterozoic Transition Lee R. Kump Department of Geosciences, Pennsylvania State University, University Park, Pennsylvania 16802, USA. (lkump@psu.edu) The Archean-Proterozoic transition witnessed a revolution in the biosphere attendant upon the establishment of an oxygen-rich atmosphere. Perhaps for the first time, and apparently for the rest of Earth history, oxygen, the most potent of electron acceptors, became widely available to fuel aerobic metabolism and oxidative weathering of reduced materials on land. The timing for the passage of the rise of oxygen through the threshold for the cessation of mass-independent fractionation of sulfur isotopes (~ 10 -5 of the present atmospheric level) is fairly well established (ca. <strong>2.</strong>4 Ga). However, the reason that the atmosphere was anoxic in the Archean and oxygenated thereafter is not conclusively known. We have hypothesized that the transition to an aerobic biosphere was effected by a reduction in the volcanic sink for oxygen driven by a shift from a predominance of submarine volcanism to a more equal expression of both subaerial and submarine volcanism, itself a result of the stabilization of continents at the end of the Archean. In addition, we have discovered what may be the largest negative carbon isotope excursion of Earth history, occurring at the end of a ~ 400 m.y. interval of atmospheric oxygen rise (at ~<strong>2.</strong>0 Ga), and possibly reflecting the initial deep oxidative weathering of Archean and Paleoproterozoic organic-rich sedimentary rocks exposed on land. This oxidative weathering event may also be linked to the generation of the Oklo natural fission reactors and the widespread supergene enrichment of iron ores at this time. Platform Geosciences, Swiss Academy of Science, SCNAT Swiss Geoscience Meeting 2011 5 Plenary Session
Page 1 and 2: Abstract Volume 9 th Swiss Geoscien
Page 3 and 4: 9 th Swiss Geoscience Meeting, Zuri
Page 5: Participating Societies and Organis
Page 9 and 10: REFERENCES Alvarez, L. W., F. Alvar
Page 11 and 12: Platform Geosciences, Swiss Academy
Page 13 and 14: POSTERS «Global & Planetary» 1.A.
Page 15 and 16: 1.1 Unravelling of continued magmat
Page 17 and 18: 1.3 A simple thermo-mechanical shea
Page 19 and 20: dismembered and partly underplated
Page 21 and 22: 1.6 Causes of single-sided subducti
Page 23 and 24: Figure 3. Simulation snapshots of a
Page 25 and 26: pected formation temperature. The r
Page 27 and 28: 1.12 Spatial distribution of quartz
Page 29 and 30: The lateral continuity of the Helve
Page 31 and 32: Figure 1. Schematic block diagram (
Page 33 and 34: 1.16 Thermal evolution in a spheric
Page 35 and 36: Figure 2: Simulations with multiple
Page 37 and 38: Figure 1. Top: Schematic map of nor
Page 39 and 40: Late Precambrian Late Cambrian - Ea
Page 41 and 42: REFERENCES Bunte, M.K., Williams, D
Page 43 and 44: pressures, deformation by interstic
Page 45 and 46: Figure 2. Determination of the temp
Page 47 and 48: 1.B.2 Long term evolution of subduc
Page 49 and 50: 1.B.4 Decoupled and coupled multile
Page 51 and 52: with time (c) 7.2 Myr and (d) 13.5
Page 53 and 54: 1.C.2 Plastic deformation of quartz
Page 55 and 56: 1.C.5 Mechanics of kink-bands durin
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1.C.8 Grain size evolution in 2D nu
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Figure 1: Tectonic Map of the Fribo
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Figure 1: Geographical location (N
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1.D.5 Dextral movements between the
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ding aftershock distribution that t
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Figure 1: Lateral facies variations
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There are no 3D numerical studies w
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Figure 1. The Doruneh fault satelli
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Table 2. Specific Activity of urani
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nism on Earth, which forms very sma
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REFERENCES Simoes, M. and Avouac, J
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REFERENCE: Aridhi K., Ould Bagga M.
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1.E.9 Direct versus indirect thermo
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Figure 1: Schematic tectonic map of
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POSTERS: P 2.1 Arlaux Y., Poté J,,
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2.1 C-O-H solubility under reduced
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largest partial molar volume compon
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REFERENCES Bonev, I. 2007: Crystal
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REFERENCES Antignano, A. & Manning,
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2.9 Percolation and impregnation of
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2.11 Fluid chemistry and fluid-rock
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A pile of up to 7000 m of volcanic
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2.15 Fluid composition and mineral
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Caucasus, close to the Iranian bord
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2.19 Application of high-precision
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lish the possible reaction path for
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P 2.4 Stratigraphy and sedimentolog
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P 2.6 Geology of Piz Duan: an ocean
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Figure 2. Summary of LA-ICPMS conco
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P 2.9 New age constraints on the op
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P 2.11 The influence of bulk and mi
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P 2.13 Petrographic and sedimentolo
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P 2.15 The Petrology and Geochemist
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Peridotites from the Dehshekh Massi
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REFERENCES Conticelli, S., Guranier
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P 2.21 Stratigraphic successions in
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Aknowledgement This study was suppo
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Water-settled pyroclastic fall depo
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P 2.26 Main Features of the Tectoni
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Figure 1. (A and B) Reconstruction
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P 2.29 The coupling of deformation
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P 2.31 When did the large meteorite
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3.1 Late Albian Carbon Isotope Stra
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3.3 Solution speciation controls me
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3.5 Clumped isotope analysis of Poz
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REFERENCES Erickson, B.E., & Helz,
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Extreme events such as destructive
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REFERENCES Archer, C. & Vance D., 2
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P 3.1 A volcanically induced climat
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P 3.2 In the Tethys Ocean black sha
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Swiss Geoscience Meeting 2011 Platf
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POSTERS: P 4.1 Broderick, C., Schal
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4.2 The importance of visco-elasto-
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4.4 Andesite production in a deep c
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4.6 Petrologic consequences of vari
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ages of the NE-Adamello with the Mi
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The example of the Adamello batholi
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4.12 Fluid evolution of the Monte M
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4.14 Magma Emplacement Tectonics: W
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P 4.2 2D numerical modelling of flu
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P 4.4 Trace-element partitioning in
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REFERENCES Hamilton, M.A., Pearson,
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P 4.8 Textures and chemistry of zir
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REFERENCES Bindeman I. 2008 Reviews
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P 4.11 Field relations and conseque
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5.1 Quaternary Geologic Map of Osog
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5.4 Tectonics, Climate, and Mountai
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Intense rainfall events may trigger
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P 5.1 InSAR Terrasar-X visibility a
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P 5.3 Landscape Evolution of the H
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Most of the other factors like slop
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P 5.8 Crack air convection and resu
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POSTERS P 6.1 Brönnimann D., Ismai
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6.2 Stalagmite evidence for a highl
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6.4 Nature and Timing of Terminatio
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6.6 Fluid inclusions in stalagmites
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6.8 Paleoenvironmental changes in e
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6.10 The recurrence pattern of mega
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6.12 Exposure ages from erratic bou
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6.14 Phylogeographic and morphologi
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We thank the ELEMO Scientific Progr
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P 6.4 Preliminary archeomagnetic re
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Anisotropy of magnetic susceptibili
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Table 1- Quaternary Chronostratigra
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P 6.10 A multidisciplinary approach
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like tsunami. Further detailed stud
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8.1 Respiration and microbial dynam
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8.3 Water management and allocation
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Figure 1: Glacier de la Plaine Mort
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8.6 Karst system characterization (
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cess points to the groundwater. Add
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8.10 Real-time spatiotemporal combi
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REFERENCES Barnett T., J.Adam, and
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P 8.1 Effect of climatic forcing on
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P 8.2 Impact of the uncertainty in
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REFERENCES Farinotti, D., S. Usselm
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REFERENCES GRETILLAT, P.-A., 1992 :
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POSTERS P 9.1 Alig C., Mitterer C.,
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We could show that both a critical
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9.5 Recent glacier changes in the A
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9.8 Seismological Experiments on th
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tive sites. Analyzing more samples
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P 9.1 On the reliability of indicat
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Figure 1. Overview of the study reg
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The internationally coordinated col
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REFERENCES Bahr, D. B., M. F. Meier
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P 9.10 Stability information suppli
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Figure 1. Resistivity - temperature
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P 9.13 The first complete inventory
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P 9.16 Monitoring temporal changes
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9.18 Study of a new Svalbard ice co
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P 9.20 Glacier Laser-scanning Exper
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10.1 Numerical simulations of short
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10.3 New balloon sounding technic u
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10.5 Radiation errors and uncertain
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P 10.1 A simple statistical model f
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12.1 Dust analysis in human lungs K
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Figure 2: concentration of selected
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The examined particles range from 2
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Figure 1. Comparison of the cytotox
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P12.2 Sediments size characteristic
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POSTERS: P 14.1 Costeur L., Domenic
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14.2 Palaeoenvironmental reconstruc
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Our results suggest that oceanograp
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14.5 Biogeographic morphological in
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Considerable amounts of the platfor
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14.8 Recovery Patterns of Chondrich
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14.10 Terrestrial ecosystems during
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P 14.1 A Cretaceous fish takes a fa
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The site “Les Plantées” is sit
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P 14.4 Mining morphological evoluti
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Knappertsbusch, M., 2004 - 2009: Mo
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P 14.7 The Exogyra aquila Marls (Lo
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P 14.8 Pushing life to the extreme:
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15.1 Managing authentication and pe
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15.3 GIS-based modeling for landsli
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15.5 Earth Modeling Seen from a Mul
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Figure 1 Current progress on develo
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Fig.1: Numerical Model of the basin
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15.9 Numerical modelling for risk s
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Results The resulting dataset inclu
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A passive seismic acquisition campa
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16.1 Investigating variations of gr
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16.3 Retrieval of the ECV „snow s
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16.5 Fusion of Digital Elevation Mo
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Figure 2. Comparison of displacemen
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P 16.3 Consistent Trends in Water V
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Figure 1. Melting snow observed in
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Random selection Active selection S
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17.1 Station velocities in Switzerl
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Figure 2. System prototype housed i
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17.5 Gravity Field Determination at
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REFERENZEN Brockmann, E., Grünig,
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P 17.1 Permanent monitoring of rock
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Figure 1.Time series of 2-hour solu
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18.1 Automatic identification of fo
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3D reference data is measured manua
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ing 3D-matrices for each flight tra
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Until now, most (semi)-automated sp
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REFERENCES: Angert, A., Biraud, S.,
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cy from these products requires cor
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This contribution reports on curren
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20.1 Prospects of Deep Geothermal E
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20.3 Deep geothermal systems - adva
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20.5 Enhanced Geothermal Systems (E
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20.7 Process simulation: understand
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20.9 Key success factors for Enhanc
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We estimate stress drops of the ind
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P 20.4 Changes of Coulomb Failure S
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P 20.6 Geothermal energy potential
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21.1 Macroscopic Source Properties
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Attenuation arises due to induced p
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nuous background medium. The contin
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Figure 1 The distribution of polari
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21.8 The long-term seismic cycle at
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Figure 1: The results of the gravit
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P 21.3 Toward source characterizati
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P 21.5 Physical mechanisms for low-
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Poshtkuh basin is located in Semnan
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REFERENCES Jackson, I., and M. S. P
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REFERENCES Goloshubin, G., Van Schu
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22.1 Sediment budgets and fluvial d
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Biochronologically controlled trans
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Fig. 1. Section across the N part o
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Sedimentary Petrology. 61, 1173-118
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22.8 Tectonics versus palaeoceanogr
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Eclogae Geologicae Helvetiae, v. 99
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P 22.1 The Cretaceous-Tertiary tran
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The young age of these km-sized fly
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evolution of the basin is character
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