PGP Achievements 2007 in brief PG… · his work on the book “Fjellenes historie” (the history of the mountains) in 2008. His 2006 book “Enden er nær” was pub-lished in English

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PO Box 1048 Blindern N-0316 Oslo

Norway

phone: (+47) 22 85 61 11fax: (+47) 22 85 51 01http://www.fys.uio.no/[email protected]

Annual Report 2008PGP

COVERPHOTO: Satelite image of East Greenland, showing fjords stretching from the cost and ca. 400 km westwards to the Greenland icesheet. The fjordsystem locally cuts 4 km down from the old ‘paleosurface’ and is a classical example of a fractal landscape. In a 2008 Geology paper, Medvedev, Hartz and Podladchikov presented a geodynamic model that explains how erosion caused more than 1.2 km of uplift, thereby solving a century long enigma of why Mesozoic marine rocks form high mountains in Greenland. Sateliteimage by NASA (http://visibleearth.nasa.gov/)

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PGP ISI citations

A total of 58 papers were published in Institute for Scientific Information (ISI) recognized journals. This corresponds to about 3.3 ISI papers per senior scientific staff man year. About 45% were in high-impact (top 3) journals including Nature, Physical Review Letters, Earth and Planetary Science Letters, and Geology. 39 ISI articles are currently in press or already published in 2009 by March 20. PGP has become a major player in the international science community as well as in the public domain. The numbers of invited scientific talks (48 in 2008) is limited by how many in-vitations we choose to accept. The number of contributed pre-sentations at conferences was 136 (85 at international meet-ings outside Norway) and is limited by the PGP budget. PGP scientists organized 5 special sessions and workshops at international meetings (including American Geophysical Union (AGU) in San Francisco and IGC 2008). In addition, 5 internal seminars were organized including the 21st Kongsberg seminar on ‘Fragmentation processes in the Earth’, which was attended by about 15 leading international scientists as well as PGP staff and students. PGP carried out 10 fieldtrips in 6 countries on 3 continents. The field trips included international and national collabora-tors and students.

5 students (2 PhD and 3 Masters) graduated from PGP. 24 out of the 26 students who graduated from PGP so far have full time paid jobs. 9 are working in petroleum related businesses, 10 are in academia. 7 former PGP post docs and senior re-searchers are working in academic institutions abroad.

4 Guest students visited PGP for one semester, and 15 invited scientists gave talks at PGP in 2008.

About 10 MNOK of the total 2008 budget of 42 MNOK came from externally funded projects, including 9 NFR projects and 2 projects sponsored by StatoilHydro (to PGP via NGU) and Aker Exploration.

Several PGP students received awards and recognitions in 2008. Luiza Angheluta received an ‘Outstanding student post-er award’ for her presentation at the 2007 AGU meeting in San Francisco; Torbjørn Bjørk received the prize for the best Master thesis in geoscience for 2006-2008 at the Norwegian

geological wintermeeting in January 2009; Marcin Krotkiews-ki won the best poster award at the 7th Annual meeting in high performance computing and infrastructure in Norway in May 2008, and Alban Souche who spent several months at PGP during his Masters project received an award for the best Master thesis in geology at the University of Strassbourg. Among the seniors, Trond Torsvik was elected a member of the Danish Academy in 2008 and was also elected to direct a research group at the Center for Advanced Studies at the Nor-wegian Academy of Science and Letters in 2010-2011. Fran-cois Renard received the prestigious ‘Institute Universitaire de France’ award, and PGP postdoc Christophe Raufast received the French Rheological Associations prize for best PhD thesis in November 2008

PGP Achievements 2007 in brief

2 PGP Annual Report 2008PGP Annual Report 2008 PGP Annual Report 2008

PGP Achievements 2008 in brief............................................ 2

Directors comments ................................................................. 4

Physics of Geological Processes .............................................. 5Mission Statement ................................................................. 5Main Challenges ...................................................................... 5Aim ............................................................................................. 5

Scientific status – Main projects ............................................ 6A. Geodynamics ........................................................................ 7B. Fluid processes................................................................... 16C. Localisation processes...................................................... 32D. Microstructures.................................................................. 38E. Interface processes ......................................................... 44

Education ................................................................................... 52

Petromax and Industry funded projects .............................. 54

Public relations ......................................................................... 55

Organisation ............................................................................ 56

Infrastructure and laboratories ............................................ 59

Finances ..................................................................................... 61

Appendices ............................................................................... 63List of staff .......................................................................... 64Student list ........................................................................... 66Numerical models ................................................................. 68Registered field work .......................................................... 69Project portfolio .................................................................. 69Invited talks 2008 ................................................................. 72Experimental laboratory activities .................................... 72Production list ....................................................................... 74

Table of Contents

PGP Annual Report 2008PGP Annual Report 2008 3

PGP. 24 of these are in paid jobs. 9 are working in petroleum companies or in companies doing petroleum-related busi-ness, 10 remain in academic environments.

PGP continued to receive a high level of media coverage in 2008 including continued coverage of our studies of the Lusi mud volcano in Indonesia. Interviews with PGP research-er Adriano Mazzini have been published in a wide range of media including: radio interviews by BBC and Dradio-Deutschlandfunk, aricles in Geoscientist, Geotimes, New Scientist, National Geographic, Süddeutsche Zeitung, and a large number of online newspapers and magazines.

PGP researchers launched two new popular book projects in 2008. Henrik Svensen received a grant from the Norwegian Non-Fiction Writers and Translators Association to support his work on the book “Fjellenes historie” (the history of the mountains) in 2008. His 2006 book “Enden er nær” was pub-lished in English in 2008 (with the title “The End is Nigh: A History of Natural Disasters”). The second book project “Reisen til istiden” (The journey to the ice age) is based on a fieldtrip to Greenland with part-time PGP-geologist and project leader Ebbe Hartz, his collaborator Niels Hovius (University lecturer at Cambridge University) and their sons Torjus and Miro. The book has been accepted as ‘hovedbok’ (main book) by Den norske Bokklubben, which will secure a broad distribution in Norway. Moreover, the expedition to Greeland will be covered through 5 episodes of the popular NRK-TV science program Newton.

PGP-Art from the geo-pattern inspired exhibit ‘Geoprints’ by ‘our’ artist Ellen Karin Mæhlum was displayed at the 33rd International Geological Conference at Lillestrøm in August. A new exhibit by Mæhlum, inspired by compaction experi-ments, was opened in one of our own laboratories.

To prepare for the post CoE periode, it is now PGP’s strategy to expand our project portfolio from EU, the industry, and other external sources. We also encourage initiation of proj-ects with visible relevance towards energy and environment. This is reflected by our most recent major projects: Two EU-projects started, or was granted, in 2008. The EU Network project ‘Delta-min’, includes Haakon Austrheim, Bjørn Jamt-veit, and two new PhD students (Jörn Hövelmann and Oliver Plümper). Our new postdoc, Julien Scheibert, received an EU

PGP is in its last half. The output of our main product, high quality papers has risen strongly during the last three years. From a level of 20-25 PGP-papers in Institute for Scientific Information (ISI-) journals during the first couple of years, we are up to 58 in 2008. About 50% of these are in the top physics and earth sciences journals (in terms of impact factor), includ-ing 1 in Nature, 1 in Nature physics, 1 in Reviews in geophys-ics, 1 in Annual Review of Fluid Mechanics, 3 in Geochimica et Cosmochimica Acta, 3 in Geology, and 11 papers in Earth and Planetary Science Letters. A Nature geoscience paper was furthermore published in February 2009.

Although 80% are published in earth science journals (and 20% in physics), we consider 50% of the papers to be truly cross disciplinary in the sense that they are based on a com-bination of competences that cannot be found in a traditional discipline-oriented research group. About 25% of all papers are co-authored by both geoscientists and physicists, and many of those produced by geoscientists only are co-authored by both field geologists and ‘modelers’.

The papers produced by PGP staff in the period 2003-2008 are on average cited about 3,5 times per year. This is very satis-factory for any branch of Earth Sciences, and in particular for cross-disciplinary research which tends to be cited less than the more established disciplines.

PGP continues to produce young researchers for the interna-tional academic market. Senior researcher Stephane Santucci left at the end of 2008 to take on a permanent CNRS position at ENS Lyon, and postdoc Timm John accepted an assistant professor position at the University of Münster. Former post-doc Espen Jettestuen got a position as researcher at IRIS (the International Research Institute of Stavanger). He will how-ever, keep an adjunct researcher positon at PGP.

Among our students, Marcin Dabrowski continues as a post-doc and group coordinator at PGP after having received his PhD in June. Evgeny Tanzerev finished in September and ac-cepted a postdoc position at NTNU. Three Masters students graduated in October. Yngve Ydersbond now works with in the company Kjeller vindteknikk AS, Munib Sarwar has been engaged in a short term contract with PGP, whereas Ola Erik-sen works for the company Volcanic Basin and Petroleum Re-search. By the end of 2008, 26 students have graduated from

Director’s comments


Mission StatementOur mission is to obtain

• a fundamental and quantitative understanding of the Earth’s complex patterns and processes

• efficient ways of transmitting our basic research to the educational system, the industry and the public

Main ChallengesOur main challenges are

• establishing an adequate conceptual framework for dealing with the Earth’s complex materials and pro-cesses

• attracting highly qualified national and international scientists and students

AimOur aim is to establish an interdisciplinary science centre that includes scientists from the fields of Physics, Geology, and Applied Mathematics

• where geological processes are approached by inte-grated fieldwork, experiments, theory and computer modelling

• with an active and challenging program for master students

• with active support from commercial enterprises, national and international foundations, and public agencies

Physics of Geological Processes

Marie Curie grant for his project ‘Earthcracks’ in collabora-tion with Dag Dysthe and others at PGP. Paul Meakin and collaborators got a major grant for the project ‘Mechanism of primary migration’ from NFR’s PETROMAX program, whereas Torgeir Andersen and others got funding from VISTA for the project ‘thermal evolution of sedimentary basins above large shear zones and detachments’. Alban Souche is a new PhD student in this project. Two new PhD’s were funded directly from UiO: One in a collabora-tive project on CO2-sequestration between Haakon Aus-trheim and Per Aagaard at the department of geosciences in Oslo. Andreas Beinlich started his PhD on this project in September. Marcin Krotkiewski received a PhD to work with Dani Schmid and collaborators from CMA (Center for Mathematics of Application), another CoE in Oslo.

During its first 6 years of existence, PGP has grown into one of Europe’s leading research groups focusing on fun-damental geological processes. Our prime goals are to con-tinue our cross-disciplinary crusade to provide quantitative understanding of how the Earth works and to produce stu-dents with a unique competence to address problems of relevance for both science and society.


Scientific status – Main projects

IntroductionFrom August 2006 PGP merged previous research activities into five main projects: Interface processes, the dynamics of microstructures, localization processes, fluid processes, and the dynamics of plate margins. The coupling between fundamental processes across various time and length scales plays an important role in almost all natural systems. The linkage across scales leads to the emer-gence of spatial and temporal patterns, as cooperative phe-nomena. A comprehensive understanding of these phenom-ena is essential if we wish to explain the behaviour of systems with natural complexity, and develop ways of predicting and controlling their behaviour to protect the environment, secure natural resources and assess natural hazards.

Schematic diagram illustrating the linking between the 5 core projects and the ‘scale independent’ role of fluids. 1) Stress induced macrosteps on a NaClO3 crystal surface coarsen in time, resulting in an unstressed skin and this has mechanical strengthening implications for larger-scale deformation processes. 2) Finite element simulation of exsolution and microstructural evolution in feldspar. 3) 3D finite element calculation of the deformation, interaction, and bulk properties in a system of particles in a matrix of another phase. 4) Deformation, strain partitioning, and clast interaction in high strain shear zone (mylonite). 5) Anastamosing deformation bands formed in porous sandstones are strain hardening, brittle faults that strongly influence mechanical stability and fluid flow. 6) Thermal structure, volcanism and fracturing in a subduction zone. 7) Large scale fracturing (image ≈20 meters across) with associated fluid migration, mineral reactions and metamorphism of initial rock from granulite to amphibolite.

Figure 1 shows how the five core projects are linked, with some of the most important feedbacks between the four scales. Fluids are unique in the sense that they play a key role at all scales – sometimes merely as a transport medium or agent, and sometimes as a chemically active ingredient. The coupling across scales and the role of fluids are common denominators in the PGP research activities. The activities within the five core groups are described below.


Figure A1. Continental Drift through Plate Tectonics to Mantle Dynamics: Reconstruction of Pangea (c. 300 Ma) according to (a) Wegener (1915; relative fit with Africa fixed), (b) Torsvik & Cocks (2005; palaeomagnetic reconstruction without longitudes), and (c) Torsvik et al (2008c) based on the hybrid absolute reference frame (Torsvik et al. 2008b) in which longitudes are ‘known’. We show the latter together with Large Low Shear wave Velocity Provinces (LLSVPs) at the core-mantle-boundary (CMB). Our reconstruction in the hybrid frame suggests that all large igneous provinces (LIPs), incuding. the 300 Ma Skagerrak centered LIP (yellow star), are caused by deep plumes that originated from the margins of the LLSVPs, near the thick white line, at the CMB.

1. Towards a global reference frame linking plate motions and processes in the deep Earth interior

A. Geodynamics

Integration of plate tectonics and mantle dynamics requires first of all that we know the palaeo-motions of the plates and can thus reliably reconstruct plate positions through time. We analyzed several different reference frames and for the first time developed a unifying approach for connecting a hotspot track system and a paleomagnetic absolute plate reference sys-tem into a ‘hybrid’ global model for the time period from the assembly of Pangea to the present. For the last 100 Ma we use a moving hot spot reference frame that takes mantle convec-tion into account, and we have connected this to a pre–100 Ma global palaeomagnetic frame adjusted 5o in longitude to smooth the reference frame transition (Torsvik et al. 2008a).

Motion of continents relative to the Earth’s spin axis may be either due to motion of individual continents or due to ro-tation of the entire Earth relative to its spin axis: True Po-lar Wander (TPW). We have therefore devised two different plate motion reference frames: one without correction of TPW (Torsvik et al. 2008a) to be used in classical palaeogeographic reconstructions and one with TPW correction. Steinberger & Torsvik (2008) developed a novel approach to determine TPW by computing the global average of continental motion and rotation through time in a palaeomagnetic reference frame. In this way, they were able to separate motions with the charac-teristics of TPW (“stop-and-go” motions, in particular coher-ent rotations of all continents around a point close to their common centre of mass) from those motions characteristic for continents moving over the underlying mantle (gradual and slowly changing over long times).


A. Geodynamics

Using plate-driving force arguments and the mapping of re-constructed Large Igneous Provinces to Core–Mantle Bound-ary topography (Torsvik et al. 2008b,c) we can for the first time link plate reconstructions to mantle geodynamic models as far back as Pangea times. A reliable plate motion reference is also important and in many cases critical for improving un-derstanding in fields as diverse as palaeogeography, palaeobi-ology, long-term environmental evolution, tectonics and Earth history on the grandest scale.

References

Steinberger, B., Torsvik, T.H. 2008. Absolute plate mo-tions and true polar wander in the absence of hotspot tracks. Nature, 452, 620-623.

Torsvik, T.H., Cocks, L.R.M., 2004. Earth geography from 400 to 250 million years: a palaeomagnetic, faunal and facies review. Journal Geol. Soc. Lond. 161, 555-572.

Torsvik, T.H., Müller, R.D., Van der Voo, R., Steinberger, B. & Gaina, C., 2008a. Global Plate Motion Frames: Toward a unified model. Reviews of Geophysics, 46, RG3004, doi:10.1029/2007RG000227.

Torsvik, T.H., Steinberger, B., Cocks, L.R.M., Burke, K. 2008b. Longitude: Linking Earth’s ancient surface to its deep interior. Earth Planet Science Letters, 276, 273-283.

Torsvik, T.H., Smethurst, M.A., Burke, K., Steinberger, B. 2008c. Long term stability in Deep Mantle structure: Evidence from the ca. 300 Ma Skagerrak-Centered Large Igneous Province (the SCLIP). Earth Planetary Science Letters 267, 444-452.

Wegener, A. 1915. Die Entstehung der Kontinente und Ozeane.


for future investigations of mantle processes focused on the lithosphere (Beuchert and Podladchikov, 2009b).

Whereas stability of cratonic keels can be explained from large viscosity ratios, stability of the boundary layer at the base of the mantle, LLSVPs (Figure A1c) cannot be due to high vis-cosities. Instead, the viscosities inside LLSVPs are presumably lower than in the surrounding lower mantle due to existence of melt fractions (e.g., Lay et al., 2006) and/or increased iron content. Although the gravitational stability of LLSVPs can be explained from the increased density of LLSVP material, as evidenced from geophysical investigations, the dynamic stability of low viscous LLSVPs under the influence of vigor-ous mantle convection is still to be explained. To this end, we conducted mantle convection simulations where we model LLSVPs as dense, low viscous material with the transition be-tween surrounding mantle and LLSVPs being a phase bound-ary between solid and partially molten material.

Our modeling results show that LLSVPs can remain stable and that their steep-sided shape and coherence can be dy-namically sustained due to cold downwellings to the sides of LLSVPs (Figure A4). These downwellings sweep the dense, low viscous anomalies into piles. The resistance to mixing of LLSVP material with the surrounding mantle is alleviated due to (i) effective decoupling between low viscous anomalies and surrounding mantle and (ii) the fact that we assume a phase boundary between solid surrounding mantle and par-tially molten material inside LLSVPs. Thus, flow can penetrate through this phase boundary without significantly disturbing the shape of LLSVPs.

Whereas we observe stability of LLSVPs at the base of the mantle in our numerical model, we found a pronounced lack of lateral stability of LLSVPs. This is in apparent contrast to the observation that the two pronounced LLSVPs under Af-rica and the Pacific remained near the equator, i.e. laterally stable, over long geological times (Figure A1c). The lack of lateral stability of LLSVPs in our numerical model indicates that an additional, equatorward directed force is required to explain long-term near-equatorial (i.e. lateral) stability of LLSVPs. We suggest that centrifugal forces can account for collection of an anomalously dense, low viscous material and subsequent stabilization of LLSVPs near the equator. We sup-port our suggestion by an open channel flow approximation in which dense LLSVPs material can flow towards the equa-tor under the influence of centrifugal forces in relatively short time given realistically low viscosities (Beuchert and Podlad-chikov, 2009a).

ModelsWe investigated the stability of boundary layer anomalies of the Earth’s mantle under conditions of vigorous convec-tion. Geophysical studies have revealed the existence of pro-nounced shear wave velocity anomalies both in regions at the top and bottom of the mantle. At the cold top boundary, Archean cratons exhibit positive shear wave anomalies down to depth exceeding 200 km, suggesting anomalously low tem-peratures in cratonic keels. Archean cratons contain all of the major diamond deposits on our planet. Dating of diamond in-clusions from Archean kimberlite pipes yielded Archean ages for the formation of the diamonds, meaning that Archean lith-osphere has been cold and stable ever since its formation in the Archean. These petrological evidences have recently been questioned based on evidence of craton instability in numeri-cal mantle convection models.

We devised a new, dynamic thermal Finite Element Method (FEM) mantle convection model and apply more realistic vis-cosity ratios between the cold, rigid lithosphere and the hot sublithospheric mantle. Our assumptions about realistic vis-cosity ratios are based on extrapolation of results from labo-ratory experiments to the low temperatures inside cratonic keels. Previous models have applied only moderate viscosity ratios, resulting in unrealistically soft model cratons which were readily eroded by vigorous mantle convection. We show that sufficiently large viscosity ratios are needed to prevent craton erosion for long geological time and deliver a quanti-tative relationship between Rayleigh number, viscosity ratio, thickness of the initial anomaly, i.e. the model craton, and time to instability of the craton (Figure A2). The derived rela-tionship shows that cratons can be stable for billions of years when more realistic viscosity ratios are applied. In our model, we apply a viscoelastic rheology which takes into account that the lithosphere behaves elastically on geological times where-as the sublithospheric mantle behaves like a viscous fluid. We found no significant difference between viscous and viscoelas-tic models for the question of craton stability (Beuchert et al., 2009).

Yet, stress fields inside the lithosphere differ significantly be-tween viscous and viscoelastic rheologies (Figure A3). Thus, if accurate stresses are to be predicted inside the lithosphere in dynamic mantle convection simulations, a viscoelastic rheol-ogy is required. Computation of accurate stress distributions is essential when more realistic, stress-dependent processes like power law creep, shear heating and plasticity are to be explored. Our newly developed incompressible viscoelastic FEM convection code will thus serve as an important tool

A. Geodynamics

2. Stability of Boundary Layers in Turbulent Mantle Convection


A. Geodynamics

Figure A2: (a) Phase diagram for upper mantle convections. Filled circles: Model craton stable for > 1 b.y., crossed, open circle: craton unstable within 1 b.y. Color contours show the time to instability tunstable (logarithm of years). From these results and those for whole mantle simulations, we derived a quantitative relationship between Ra is the Rayleigh number, μr is the viscosity ratio and δc the ratio of domain height to thickness of the anomaly, i.e. the craton. The data fit is given in (b) by red curve. The fit holds both for viscous (open circles) and viscoelastic simulations (points).

Figure A3: Distribution of effective stress (right) in a thermal convection (temperature field shown on the left) simulation of the upper mantle (660 km) after 100 m.y. simulation time for Deborah numbers De = 0 (viscous), 10-9 and 10-7. Bottom heating Rayleigh number Ra=2x107, exponential temperature-dependent viscosity maximum viscosity ratio μr=μ(Tmin)/ μ(Tmax)=1010. The stress distribution within the lithosphere differs substantially between viscous (De=0) and viscoelastic simulations. Increasing the Deborah number results in an increase in thickness of the elastically responding lithospheric keel. Top and bottom boundaries are zero traction (free slip) boundaries, sides are periodic (wrap-around). Temperatures are fixed at minimum and maximum values at top and bottom, respectively.


ReferencesBeuchert, M.J., Podladchikov, Y.Y. 2009a. Long-term sta-

bility of Large Low Shear Velocity Provinces (LLSVPs) at the base of the mantle and near the equator. (to be submitted to EPSL).

Beuchert, M.J., Podladchikov, Y.Y. 2009b. Viscoelastic mantle convection and lithospheric stresses. (to be submitted to GJI).

Beuchert, M.J., Podladchikov, Y.Y., Simon, N.S.C., Ruepke, L.H. 2009. Modeling of craton stability using a viscoelastic rheology. (to be submitted to GJI).

Lay, T., Hernlund, J., Garnero, E.J., Thorne, M.S. 2006. A post-perovskite lens and D ‘’ heat flux beneath the central Pacific. Science, 314(5803): 1272-1276.

Figure A4: (a) Temperature distribution after 440 m.y. of simulation time. The black contour shows the limit of partially molten material in the basal piles. Plumes are episodically emanating from the sides and top of the piles. (b) Close up view of the area indicated by the box in a). The hottest regions are located at the edges of the pile and are swept to the sides by the convective flow inside the pile. Arrows indicate flow inside the pile. The structure obtained in our numerical model is in excellent agreement with (c) structural interpretation of LLSVPs/ULVZs based on seismic data (picture modified from Lay et al., 2006). Pv: perovskite, pPv: post-perovskite.

A. Geodynamics


The joint work between T.B. Andersen (PGP) and Brad Hack-er (UCSB) on burial and exhumation of high- and ultra-high pressure rocks in the Western Gneiss Region of Norway have been going on with collaborators at University of California Santa Barbara (UCSB) commenced before PGP was estab-lished. Since 2003 this collaboration has resulted in several joint publications. A review manuscript compiled by Hacker and Andersen summarizing the results including work by two jointly supervised PhD students (David Young, PhD, UCSB 2005 and Scott Johnston, PhD, UCSB 2006) since 2003 was submitted to Tectonophysics (December 2008). The paper summarizes a wealth of data on structure, metamorphism and age-determinations from the northern part of the WGR, and presents the unified results of our joint research papers pub-lished since 2003 (Hacker et al. 2003, Johnston et al. 2007, Young et al. 2007). The paper gives an interpretation of the exhumation from 1.8 to ca 2.8 GPa eclogite corresponding to the lower stability field of coesite, not very different than the much referred by Andersen and coworkers (1991). This model does, however, not explain exhumation from diamond to majorite pressure conditions know form other studies to be present in the UHP part of the region (Vrijmoed 2009, Vrij-moed et al. 2006). A summary map of structure, metamorphic and some of the geochronological data is shown in Figure A5, from Hacker et al. (submitted). Of special interest here are the UHP domains which are exposed in cores of antiformal culminations that also fold isobars (notice the trend of the 2.8 GPa isobar).

3. Work on Caledonian high and ultra-high pressure rocks in western Norway

ReferencesAndersen, T. B., Jamtveit, B., Dewey, J. F., Swensson,

E. 1991. Subduction and Eduction of Continental-Crust - Major Mechanisms during Continent-Continent Collision and Orogenic Extensional Collapse, a Model Based on the South Norwegian Caledonides. Terra Nova, 3, 303-310.

Hacker, B. R., Andersen, T. B., Johnston, S., Kylander-Clark, A., Peterman, E., Walsh, E., Young, D. Deforma-tion during continental margin subduction and exhu-mation: The Ultrahigh-Pressure Western Gneiss Region of Norway. Tectonophysics (Submitted).

Hacker, B. R., Andersen, T. B., Root, D. B., Mehl, L., Mattinson, J. M., Wooden, J. L. 2003. Exhumation of high-pressure rocks beneath the Solund Basin, West-ern Gneiss Region of Norway. Journal of Metamorphic Geology, 21, 613-629.

Johnston, S., Hacker, B. R., Andersen, T. B. 2007. Exhum-ing Norwegian ultrahigh-pressure rocks: Overprinting extensional structures and the role of the Nordfjord-Sogn Detachment Zone. Tectonics, 26, TC5001, doi:10.1029/2005TC001933.

Young, D. J., Hacker, B. R., Andersen, T. B., Corfu, F. 2007. Prograde amphibolite facies to ultrahigh-pressure transition along Nordfjord, western Norway: Implica-tions for exhumation tectonics. Tectonics, 26, TC1007, doi:10.1029/2004TC001781, 2007.

Vrijmoed, J. C. 2009. Physical and chemical interaction in the interior of the Caledonian mountains of Norway University of Oslo. Unpublished PhD thesis, 200 pp.

Vrijmoed, J. C., Van Roermund, H. L. M., Davies, G. R. 2006. Evidence for diamond-grade ultra-high pressure metamorphism and fluid interaction in the Svartber-get Fe–Ti garnet peridotite–websterite body, Western Gneiss Region, Norway. Mineralogy and Petrology, 88, 381-405.

A. Geodynamics


Figure A5. Map of the study area in the northern part of the Western Gneiss Region. Color shades grey to green shows increasing (dark green) intensity of the Caledonian deformation. The western parts and the area adjacent to the Caledonian nappes and near the Nordfjord-Sogn Detachment zone are more intensely deformed. Eclogite facies isobars increase westwards from the first appearance of eclogites (ca 1.8 GPa) to the ultrahigh-pressure domains (>2.8 GPa). Notice also that the sphene ages are reset to late Caledonian ages in the west and that precambrian sphene ages are pervasively preserved in the southeast. The UHP domains are defined by mapping in the project and by Vrijmoed et al. (2006).

A. Geodynamics


A. Geodynamics

Results of PGP research on blueschist and eclogite facies pseudotachylytes in the Alpine parts of Corsica has been pub-lished in 2 previous papers (Andersen & Austrheim 2006, Austrheim & Andersen 2004). A new study was published in Geology in 2008 (Andersen et al. 2008). This study uses very small faults with constrained minimum displacement and dec-orated by thin films of ultramafic pseudotachylyte to constrain the stress during seismic faulting that formed the pseudotahy-lyte. The results show that near complete adiabatic melting of the spinel and plagioclase lherzolites took place during the faulting (Figure A6). This joint PGP effort has uncontro-vertably show that mantle lithosphere is able to sustain very large stresses during subduction/collision. We have demon-strated that stress-drops of more than 5.8 kbar were released by earthquakes at intermediate depth (≥1.5 GPa). These mini-mum stresses were obtained by calculating the minimum re-lease of energy that goes into formation (heating + melting) of pseudotachylytes along faults with known minimum displace-ments (Figure A6). The textures of the quenched melts in the pseudotachylytes also demonstrate that static crystallization took place after the faulting, implying that very low stresses was present in the rock and more or less complete stress-drop during the co-seismic faulting.

The work on the Corsican pseudotachylytes has been carried out as a collaboration between the geodynamic and localiza-tion group, and the results of the stress determinations have already been used in new work by PGP researchers on mecha-nism of intermediate to deep earthquakes (John et al. 2009). The work continues in 2009 with focus on the petrology of the ultramafic pseudotachylytes.

4. Stress-drop determinations from subduction related palaeoearthquakes in mantle rocks from Alpine Corsica

ReferencesAndersen, T. B., Austrheim, H. 2006. Fossil earthquakes

recorded by pseudotachylytes in mantle peridotite from the Alpine subduction complex of Corsica. Earth and Planetary Science Letters, 242, 58-72.

Andersen, T. B., Mair, K., Austrheim, H., Podladchikov, Y. Y., Vrijmoed, J. C. 2008. Stress release in exhumed intermediate and deep earthquakes determined from ultramafic pseudotachylyte. Geology, 36, 995-998.

Austrheim, H. K., Andersen, T. B. 2004. Pseudotachy-lytes from Corsica: fossil earthquakes from a subduc-tion complex. Terra Nova, 16, 193-197.

John, T., Medvedev, S. Rüpke, L., Andersen, T. B., Podladchikov, Y.Y., Austrheim, H. 2009. Generation of intermediate-depth earthquakes by self-localizing thermal runaway. Nature Geoscience, 2, 137-140


A. Geodynamics

Figure A6. (A) Small fault cutting gabbro vein in peridotite with measurable minimum displacement. Notice drill sampling of fault rock in the peridotite ca 20 cm from the gabbro vein. (B) Micrograph of fractured and melted (dark brown to black material) along micro-fault-strands in the peridotite.Samle from drill core in a. (C) EBS image of small pseudotachylyte fault and injection vein from the peridotite. (D) Detail of new-formed olivine dendritic crystals growing from the melt in small fault vein.


Central Scientific ProblemGases are produced when sedimentary rocks are heated by magmatic intrusions. For instance in the Salton Sea area in southern California, sediment degassing is an active process occuring today, and has been used as a field site for PGP the last seven years. Ongoing studies focus on time series analy-sis of temperature at hydrothermal seeps, and the fluxes of greenhouse gas emissions. On a larger scale, sill intrusions and short-lived hydrothermal systems are common in many sedimentary basins, forming the sub-volcanic part of Large Igneous Provinces. If vented to the atmosphere, these gases can trigger global warming periods and even more severe en-vironmental effects like mass extinction episodes. We wish to determine how gases such as water vapor, carbon dioxide, methane, and more complex compounds are produced and vented during episodes of Large Igneous Province formation. This project is particularly relevant to future climate change because the rates and volumes of gases released from hydro-thermal systems are comparable to anthropogenic greenhouse gas emissions. Understanding the gas production processes around magmatic bodies is also important for the oil and gas industry for improving the economic exploitation of hydrocar-bon reservoirs.

Recent ResultsThe most severe mass extinction in the history of life on Earth occurred at the end of the Permian period, 250 million years ago. Coeval with this event are the massive eruptions of the Siberian Traps. How exactly the Siberian traps are connected to the extinction event has now been elucidated through a study conducted by Henrik Svensen and collaborators (Svens-en et al. 2009). The Siberian Traps Large Igneous Province emplaced sill intrusions into a vast region (Figure B1) con-taining carbonates and evaporites deposited during earlier epochs, and matured to petroleum-bearing rocks before the sill emplacement. Metamorphic heating of these sediments resulted in the production of vast quantities of volatiles that were eventually released to the surface, leading to abrupt and significant effects on the global climate. Field expeditions to Siberia’s Tunguska basin in 2004 and 2006 collected samples

Introduction 1. Venting and climate effects

The Fluid Processes group at PGP continues the activities from previous years in partly overlapping subjects of vent-ing and climate effects, fluidised systems, pockmarks, sill em-placement, and violent processes. These will be discussed in more detail below. Each of these has links to other groups at PGP: sill emplacement and fluidised systems with interface processes; violent processes with localisation and fragmenta-tion; venting and climate effects with large-scale dynamics. We are large users of the Norwegian computing infrastructure system through the NOTUR project, have published a score of scientific papers, and participated in a variety of international conferences.

B. Fluid processes


Figure B1 Geological map of the Tunguska Basin in Eastern Siberia, Russia, showing the distribution of of phreatomagmatic pipes with magnetite in the south and with basalt in the north. Our main study area during a 2004 field campaign is indicated by the star symbol. The Cambrian evaporite comprises a total area of 2 million km2.

B. Fluid processes

Surkov et al., 1991; Sokolov et al., 1992). The Tunguska basin (Fig. 1) ispetroleum-bearing, with numerous reservoirs of oil and gas (Fig. 2).Carbonates and minor sandstone and shale horizons dominate theCryogenian and Tonian (formerlyRiphean) source rock sequenceswhichare overlain by the carbonate and evaporate facies of the Ediacaran(formerly Vendian). Furthermore, enormous volumes of Cambrianevaporites are present in the basin, with up to 2.5 km thick sequencesof halite-rich strata, anhydrite, and carbonates (Fig. 2) (Zharkov, 1984;Petrychenko et al., 2005). Five major phases of salt deposition occurredin the Cambrian, the most extensive being the 2 million km2 EarlyCambrian Usolye salt basinwith an average of 200 m of halite (Zharkov,1984). Note that the “Tunguska Basin” in the literature is frequentlyincluded in the terms “SiberianPlatform” and “SiberianCraton”, and thatthe TunguskaBasin is often consideredasoneofmanybasins situatedonthe platform/craton. We use the term to encompass all the post Neo-Proterozoic sedimentary rocks on the platform/craton.

The total thickness of the basin stratigraphy commonly variesbetween 3 km and 12.5 km (Meyerhoff, 1980; Kontorovich et al., 1997),however the Neo-Proterozoic rocks are locally present as 7–10 kmthick rift segment deposits (Sokolov et al., 1992; Kuznetsov, 1997;Drobot et al., 2004). Post-Cambrian rocks comprise carbonates, marls,

sandstones, and coal (Fig. 2), and the sedimentation terminated in thelatest Permian with the onset of Siberian Traps volcanism.

The Tunguska Basin sediments were intruded by the sub-volcanicpart of the Siberian Traps. Sills and dykes are abundant throughout thebasin, and form sheets up to 350m thick, locally comprising up to 65% ofthe stratigraphy (Meyerhoff, 1980; Fedorenko and Czamanske, 1997;Ulmishek, 2001). The maximum accumulated sill thickness in theCambrian to Permian strata is 1200 m (Kontorovich et al., 1997). Thethickness of sill intrusions in the Neo-Proterozoic rocks is uncertain dueto a limited number of deep boreholes in the bulk part of the basin(Fig. 2). However, thick sills are commonly present at the base of theCambrian evaporate sequence (Kontorovich et al., 1997; Ulmishek,2001). The present day area with outcropping sill intrusions is at least1.6 million km2 (Fig. 1). The sill emplacement led to widespread contactmetamorphism of the host sediments (e.g., Kontorovich et al., 1997) andto enhanced maturation of organic matter and the formation ofmethane-rich petroleum accumulations (Sokolov et al., 1992). Themost profound results of the magma-sediment interaction are specta-cular magnetite-rich breccia pipes rooted in the Cambrian evaporites orpossibly deeper. These pipes are numerous in the southern parts of thebasin, where they are filled with up to 700 m deep and 1.6 km wide

Fig. 1. Geological map of the Tunguska Basin in Eastern Siberia, Russia. Note the high abundance of phreatomagmatic pipes withmagnetite south of latitude 64, and the numerous basalt-filled pipes north of 68°. Our main study area during a 2004 field campaign is indicated by the star symbol. The aerial extent of evaporite is from Zharkov (1984). The geological map ismodified fromMalich et al (1974), and the positions of the pipes were compiled from various sources (Malich et al., 1974; Nikulin and Von-der-Flaass, 1985; Pukhnarevich, 1986; Von derFlaass and Naumov, 1995; Ryabov et al., 2005; Ryabov, 2006). The outline of the Cambrian evaporite is from Petrychenko et al. (2005), comprising a total area of 2 million km2.

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from boreholes drilled decades previously for potash pros-pecting (Figure B2). On analysis, these samples exhibit carbon depletion in the sediments adjacent to sill intrusions, and the gas-production potential is estimated to be in excess of 10 000 gigatons carbon equivalent for the basin as a whole. Violent phreatomagmatic eruptions (Figure B3) occurred when the hot sills encountered fluids residing within the evaporite lay-ers, resulting in an outgassing much more rapid than occurred in other Large Igneous Provinces.

B. Fluid processes

(e.g., Raymond and Murchison, 1989, 1991; Galushkin, 1997; Fjeldskaaret al., 2008). This implies that the total volume of sediments affected bycontact metamorphism is equal to twice the sill volume. Note that thegas will be produced in the aureole independent of the specific type oforganic material undergoingmetamorphism (dispersed organic matter,coal beds, or petroleum). Themass conversion factors for calculating gasequivalents from carbon are 1.34 and 3.66 for methane and carbondioxide, respectively.

3.3. Dating

U–Pb analyses on two dolerite samples from the 194 borehole(sampled at 860.8 m and 868.7 m) (Fig. 2) were carried out using ID–TIMS (isotope dilution thermal ionization) and a Finnigan MAT262instrument at the Department of Geosciences in Oslo. The 20 to 30zircon grains found in each of the two samples occurred largely asfragments, locally with some preserved euhedral faces. Most grainsshowed some local turbidity, fractures or inclusions of other minerals.Baddeleyite was only observed as an inclusion in one zircon. Abrasiongenerally removed most of the turbid parts of the fragments. The bestgrains were selected for analysis, some were perfectly clear but othersstill contained some imperfections. Zircon grains were abraded beforeanalysis, then dissolved and transferred directly to the mass spectro-meter for measurement, except for one larger fraction processedthrough anion exchange resin. A mixed 235U–205Pb–202Pb spike wasused for internal normalization of the fractionation of Pb. See Corfu(2004) for analytical procedures. The datawere calculated using decayconstants from Jaffey et al. (1971). The uncertainties are 2σ.

4. Results

4.1. The breccia

The magmatic fragments of the Scholokhovskoie pipe are rich inglass (Fig. 4), demonstrating rapid melt quenching in the pipe, and thepipe formation was accordingly contemporaneous with the sill em-placement. Hydrothermal minerals include calcite, dolomite, halite,garnet, epidote, and chlorite, either as pore filling minerals or alter-ation products from igneous fragments.

4.2. Gas generation experiments

Heating experiments on evaporite samples from the 194 boreholewere done to determine the type of gas generated during contactmetamorphism in the Tunguska Basin. We use natural rock samplesequivalent to those that were heated by sills during the end-Permian. The samples were collected at depths between 807 and949 m, including two reference samples from the contact aureole ofthe lower sill (Table 1). The samples consist of coarse grained halitewith minor sylvine, anhydrite, and pyrite. Trails of liquid and gasinclusions are abundant in the salt (Grishina et al., 1998), releasingaromatic and sulphurous gases when crushed. Table 1 show thatbutane, benzene, and sulphur-bearing gases are the most abundantof the analysed petroleum compounds at room temperature.Sulphur dioxide is identified in most samples, whereas only twosamples contain dimethyl sulphide. Note that no halocarbons weredetected.

Fig. 3. Composite cross section from the Nepa locality. The location map shows four of the Nepa boreholes that we have studied in detail and three breccia pipes. The Cambrianevaporite strata are overlain by Ordovician clastic sediments. Core data from the 6G hole in the Scholokhovskoie pipe and from the 194 hole in the lower sill intrusion are presentedhere. The topmost stratigraphic unit is Ordovician (O), and the rest of the drilled sequences are from the Late Cambrian (Verkholensk Suite), Middle Cambrian (Litvintsev Suite,abbreviated L-S), and the Lower Cambrian (Angara Suite and Bulay Suite, abbreviated B-S). The Upper sill is sometimes referred to as the Usol'e sill (Zamaraev et al., 1985).


Figgure B2 Composite cross section from the Nepa locality (star in Figure B1). The location map shows four of the Nepa boreholes that we have studied in detail and three breccia pipes. The Cambrian evaporite strata are overlain by Ordovician clastic sediments. Core data from the 6G hole in the Scholokhovskoie pipe and from the 194 hole have been analysed.


ReferencesSvensen, H., Karlsen, D.A., Sturz, A, Backer-Owe, K.,

Banks, D.A.,Planke, S. 2007. Processes controlling water and hydrocarbon composition inw seeps from the Salton Sea Geothermal System, California, USA. Geology, 35, 85-88.

Svensen, H., Planke, S., Chevallier, L., Malthe-Sørens-sen, A., Corfu, B., Jamtveit, B. 2007. Hydrothermal venting of greenhouse gases triggering Early Jurassic global warming. Earth and Planetary Science Letters, 256, 554-566.

B. Fluid processes

by our experiments. Gas generation from sediment metamorphism isknown both from the Karoo Basin in South Africa and offshore Norway,resulting in vertical piercement structures (Jamtveit et al., 2004; Svensenet al., 2004; Svensen et al., 2007). The main differences in the pipeforming mechanisms between these two settings and the one in Siberia,is the presence of evaporites and petroleum in the source region, andextensive magma-sediment interactions within the pipes. The pipes arerooted at 2–4 km depth in magma-sediment mixing zones, probably

close to the base of the evaporite stratigraphyalthough the precise natureof the roots remains unknown. Fig. 6 shows the schematic evolution ofthe pipe structures. The sizes of the pipe craters in the Tunguska Basinsuggest powerful eruptions, with gases and ash likely reaching highatmospheric levels. The presence of glass in the Scholokhovskoie brecciapipe suggests that the pipe was formed as a phreatomagmatic event,where the partly molten magma cooled rapidly in the pipe duringeruption. Parts of the wall-rock collapsed into the pipe, mixing with the

Fig. 6. Schematic evolution of the Tunguska Basin pipes and the venting of carbon gases and halocarbons to the atmosphere. The pipe evolution is partly based Von der Flaass andNaumov (1995) and Von der Flaass (1997). 1) Emplacement of sills into organic rich sediments and evaporites with petroleum accumulations (P). 2) Contact metamorphism of shale,evaporite, and petroleum, leading to gas generation and overpressure (shown as stippled lines). Melt is accumulating within evaporite sequences in the source region of the pipe. 3)Pipe formation and eruption. Glass in the breccias show that the magma was disrupted and fragmented in the source region before vertical transport and phreatomagmatism.Powerful eruptions led to wide craters and subsidence. Gases generated in contact aureoles are now released to the atmosphere. 4) Continued degassing from both magma andsediments through the pipe and the crater-lake. Contact metamorphism of shallow organic-rich sequences (coal) along dikes, and appearance of the first lava flows further to thenorth in the basin. The inferred gas composition is shown in the frame, alongside the estimated carbon gas and halocarbon production potential for the pipe degassing alone.

Fig. 7. Compilation of zircon U–Pb ages of key end-Permian events. The ages of the P–T boundary are from (Gradstein et al., 2004) deduced from Bowring et al. (1998) (stippled,labelled “B”), and from a revised age by Mundil et al. (2001) (in grey, labelled “M”). The age of the sill emplacement at Nepa (this study) is synchronous with pipe formation andrelease of carbon gases and halocarbons to the atmosphere. The main phase of the extinction is dated to have occurred between 252.3±0.3 and 251.4±0.3 Ma by Bowring et al. (1998)(labelled “B”) and 252.6±0.2 Ma by Mundil et al. (2004) (labelled “M”).


Figure B3 Schematic evolution of the Tunguska Basin pipes and the venting of carbon gases and halocarbons to the atmosphere. (1) Emplacement of sills into organic-rich sediments and evaporites with petroleum accumulations (P). (2) Contact metamorphism of shale, evaporite, and petroleum, leading to gas generation and overpressure (shown as stippled lines). Melt accumulates within evaporite sequences in the source region of the pipe. (3) Pipe formation and eruption. Glass in the breccias shows that the magma was disrupted and fragmented in the source region before vertical transport and phreatomagmatism. Powerful eruptions led to wide craters and subsidence. Gases generated in contact aureoles are now released to the atmosphere. (4) Continued degassing from both magma and sediments through the pipe and the crater-lake. Contact metamorphism of shallow organic-rich sequences (coal) along dikes, and appearance of the first lava flows further to the north in the basin.

Svensen, H., Planke, S., Polozov, A. G., Schmidbauer, N. Corfu, F., Podladchikov, Y. Y., Jamtveit, B. 2009. Siberian gas venting and the end-Permian environ-mental crisis. Earth and Planetary Science Letters, 277, 490-500.


2. Fluidised and partly fluidised systems

Central Scientific ProblemMuch of the activity in hydrothermal systems involves a phase of fluidisation, when the injection of fluid causes a portion of the surrounding matrix also to act as a fluid. Entrainment of the surrounding medium costs the initiating fluid some of its energy, but the subsequent mobilisation of material with significant inertia and limited compressibility can have impor-tant environmental consequences. This activity within PGP has recently focussed on the phenomenon of mud volcanoes. Studying these systems can provide important insights into the subsurface plumbing system and the origin of the fluids and mud breccia expelled from mud volcanoes.

Recent ResultsActive eruptions of mud volcanoes provide excellent oppor-tunities for the study of large-scale fluidisation processes in nature, and the activity of the LUSI mud volcano in Indonesia continues to be of active interest at PGP. A special issue of the Journal of Marine and Petroleum Geology with the title “Mud Volcanism: Processes and Implications”, edited by Adriano Mazzini, is now in the final stages of preparation, with many articles now in final proof form. It will be published in 2009. Contributions to this issue include observational, theoretical, and computational studies of the processes responsible for the formation and eruption of mud volcanoes and their environ-mental consequences.

The Dashgil mud volcano in Azerbaijan is the subject of a classic study of dormant mud volcanoes recently published by Mazzini and co-workers (Mazzini et al 2008). Since the erup-tive activity of mud volcanoes is generally of short duration, most of the 1500 observed world-wide are in dormant state. Even in dormant state, however, mud volcanoes continue to release water, gas and petroleum, sometimes vigorously, through seeps (Figure B4). The Dashgil mud volcano had its last eruption in 1958, and may be due for a new eruption soon, since it had been historically quite active in the 1800s. In re-cent years, activity from the seeps has fluctuated, with meth-ane and petroleum flares occurring occasionally (Figure B5). The active seep locations are coincident with caldera collapse

and other faults Detailed geochemistry and isotopic analysis suggest that gases coming from the seeps are replenished from reservoirs at considerable depth, while some of the water is meteoric and shows seasonal variations. A schematic model based on the observations is shown in Figure B6.

Another approach to the study of fluidised systems is to con-duct experiments in which fluids are injected into boxes con-taining grains with known characteristics. In a recent series of such experiments, Anders Nermoen has been injecting air into the bottom of a Hele-Shaw cell filled with grains of two dif-ferent sizes, in order to quantify the conditions of fluidisation and segregation of particles. One such experiment is illustrat-ed in Figure B7, in which air is injected at high velocity into the bottom of a mixture containing many more small grains than large ones. The permeability field depends on the local con-centration of small and large grains, being greater in regions where the large grains are more common. Air flow therefore tends to localise around concentrations of large grains, and the fluidisation brings more large grains to these locations. As a result, chimneys formed consisting mostly of large grains, and these grow towards the surface, consuming smaller neigh-bouring chimneys as they do.

Computer simulations are another way of studying fluidised systems. Galen Gisler has used the multi-material hydro-code Sage to study the break-out and eventual venting of high-pressure fluids suddenly released into a deformable and compactable medium, similar to a sedimentary basin (Gisler 2009). A sequence from one such simulation is illustrated in Figure B8, showing the medium cracking and then opening rapidly as a supercritical fluid emerges, geyser-like, from the high-pressure pipe below. The morphology of the opening vent or crater is found to depend on the pressure under which the fluid is confined at depth. At low pressures, vents are formed via diagonal cracks propagating from the break-out point and propagating relatively slowly towards the surface. At somewhat higher pressures, a straight vertical pipe forms, often accompanied by horizontal cracks, and a conical crater is formed at the surface. At still higher pressures, the pipe be-comes conical, rather than straight, and the surface eruption (as in Figure B8) is like a geyser.

B. Fluid processes


Figure B4 Satellite image of the Dashgil mud volcano, Azerbaijan, with interpreted mud flows from previous eruptions coloured and numbered in sequence from oldest to youngest. The coloured regions without numbers may be remnants of older eruptions.

Figure B5 Gryphon field inside the crater of the Dashgil mud volcano. Circled is a man, for scale. Each of these gryphons is a source of continuously seeping mud. Scattered throughout the crater are pools where gases are emitted through bubbling water.

B. Fluid processes

Fig. 2. (A) Satellite image of the Dashgil mud volcano; (B) interpreted mud flows corresponding to previous eruptions. At least three possible eruption events can be distinguished.Note: the dotted line in eruption II might represent the border between two separate events, however satellite and field observations are inconclusive to solve this ambiguity. Mudbreccia flow III represents the most recent eruption. Flows older than I cannot be excluded but cross correlations are hard to be established.

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Please cite this article in press as: Mazzini, A., et al., When mud volcanoes sleep: Insight from seep geochemistry at the Dashgil mud volcano,Azerbaijan, Marine and Petroleum Geology (2008), doi:10.1016/j.marpetgeo.2008.11.003

sample of gryphonwater from 2002 had a chlorinity of 23,900 ppm(Planke et al., 2003). Salsa lake A has Cl ¼ 13,340 ppm (versus11,457 ppm in 2002), salsa lake B has Cl ¼ 28,458 ppm (versus27,168 ppm in 2002), thus demonstrating relatively constant lake

compositions in the 4 year time span. There are, however,discrepancies in minor element composition when the 2002 and2006 data are compared (e.g., Br, B, Sr, SO4; Table 3). Also, traceelements like B and Li are enriched in the gryphons and pools

Fig. 4. Examples of the main seeping features observed in Dashgil MV. (A) Gryphons field inside the crater; (B) salsa lake A where two main venting sites are observed; (C) smallgryphon where dense mud continuously flows; (D) small pool where gas and water vigorously seep.

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B. Fluid processes

Figure B6 (A) NW–SE section of Dashgil MV. Vertical axis not to scale. The marked locations in and around the crater represent respectively: (1) The gryphon field inside the crater; (2) diffuse seepage along the outer fault margin; and (3) salsa lakes. (B) Magnification of area framed in image A highlighting the collapse controlled by faults that act as preferential pathways for the seepage of deeper fluids. At large salsa lakes deep fluids and shallow meteoric fluids converge and mix. (C) Interpreted plumbing system of gryphon-pool complex based on field observations and gas/water analyses. Overburden of the gryphons causes collapse and fractures through which the deep fluids migrate, mixing with shallow meteoric waters.

Figure B7 Fluidisation experiment with a bimodal distribution of grain sizes. Air is injected at high speed into the bottom of a Hele-Shaw cell containing a large number of small grains and a smaller number of large grains. Because a region containing more large grains than the average is more permeable, the particles tend to segregate into chimneys containing mainly large grains. They coalesce into fewer, more widely spread chimneys as they grow towards the surface.

moderate 13C depletion and higher amount of C2þ homologues arecommonly interpreted as thermogenic deep-rooted gas that risesrapidly towards the surface (e.g. Blinova et al., 2003). See Etiope et al.(in press, 2008b) for a more extensive explanation of the globalstatistics of gas seeping frommud volcanoes worldwide.

Comparison between gas sampled from the Dashgil MV andthat from the neighboring oil fields (Katz et al., 2002) gives insightabout the mechanisms of gas migration. Katz et al. (2002) show thatnumerous of the reservoir gases from the South Caspian werenot generated in situ and have been altered and/or represent mixedsource hydrocarbons. The d13CCH4 isotopic signatures of the gas

seeping at Dashgil are similar to those from deeper oil field gas (Table2). Like also pointed out by Katz et al. (2002), our results suggest thatmost of the deeper-sited thermogenic mature (?) gas migrates fromdepth greater than 3 km and that there is a negligible contributionfrom shallow biogenic methane. However the d13CCH4 of Dashgil oilfield is slightly lower than the neighboring reservoirs (Table 2) sug-gesting a small biogenic input. Similarly towhat pointed out byEtiopeet al. (inpress) ourdata also suggests that isotopic fractionation relatedtomicrobial oxidation is not significant. Yet the seeping gases (Fig. 5A,Table 2) show dramatically lower amounts of the C2 component andpresence of C3þ only in some cases and anyhow in negligible amounts

Fig. 7. (A) NW–SE section of Dashgil MV. Vertical axis not to scale. The marked locations in and around the crater represent respectively. (1) The gryphon field inside the crater; (2)diffuse seepage along the outer fault margin; and (3) salsa lakes. Symbols in the stratigraphy: PT ¼ Productive Serie-sandstones; S ¼ Sarmatian-shales; TC ¼ Tarkan–Chokrak-shales/sandstones; M ¼Maikop-shales; (B) magnification of area framed in image A highlighting the collapse controlled by faults that act as preferential pathways for deeper fluidsseepage. Seepages outside the crater show stronger d13CCO2 depletion and higher amount of CH4. At large salsa lakes deep fluids and shallow meteoric fluids converge and mix; (C)interpreted plumbing system of gryphon-pool complex based on field observations and gas/water analyses. Overburden of the gryphons causes collapse and fractures throughwhich the deep fluids migrate, mixing with shallow meteoric waters. At gryphon sites evaporation is likely to have a limited influence as gryphons contain dense mud and differmorphologically (e.g. from pools) ‘‘isolating’’ the fluids inside the crater and in the internal chambers. d18O values support a confined seepage of fluids through the feeder channelallowing a bypass through the intervals charged with meteoric fluids.

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moderate 13C depletion and higher amount of C2þ homologues arecommonly interpreted as thermogenic deep-rooted gas that risesrapidly towards the surface (e.g. Blinova et al., 2003). See Etiope et al.(in press, 2008b) for a more extensive explanation of the globalstatistics of gas seeping frommud volcanoes worldwide.

Comparison between gas sampled from the Dashgil MV andthat from the neighboring oil fields (Katz et al., 2002) gives insightabout the mechanisms of gas migration. Katz et al. (2002) show thatnumerous of the reservoir gases from the South Caspian werenot generated in situ and have been altered and/or represent mixedsource hydrocarbons. The d13CCH4 isotopic signatures of the gas

seeping at Dashgil are similar to those from deeper oil field gas (Table2). Like also pointed out by Katz et al. (2002), our results suggest thatmost of the deeper-sited thermogenic mature (?) gas migrates fromdepth greater than 3 km and that there is a negligible contributionfrom shallow biogenic methane. However the d13CCH4 of Dashgil oilfield is slightly lower than the neighboring reservoirs (Table 2) sug-gesting a small biogenic input. Similarly towhat pointed out byEtiopeet al. (inpress) ourdata also suggests that isotopic fractionation relatedtomicrobial oxidation is not significant. Yet the seeping gases (Fig. 5A,Table 2) show dramatically lower amounts of the C2 component andpresence of C3þ only in some cases and anyhow in negligible amounts

Fig. 7. (A) NW–SE section of Dashgil MV. Vertical axis not to scale. The marked locations in and around the crater represent respectively. (1) The gryphon field inside the crater; (2)diffuse seepage along the outer fault margin; and (3) salsa lakes. Symbols in the stratigraphy: PT ¼ Productive Serie-sandstones; S ¼ Sarmatian-shales; TC ¼ Tarkan–Chokrak-shales/sandstones; M ¼Maikop-shales; (B) magnification of area framed in image A highlighting the collapse controlled by faults that act as preferential pathways for deeper fluidsseepage. Seepages outside the crater show stronger d13CCO2 depletion and higher amount of CH4. At large salsa lakes deep fluids and shallow meteoric fluids converge and mix; (C)interpreted plumbing system of gryphon-pool complex based on field observations and gas/water analyses. Overburden of the gryphons causes collapse and fractures throughwhich the deep fluids migrate, mixing with shallow meteoric waters. At gryphon sites evaporation is likely to have a limited influence as gryphons contain dense mud and differmorphologically (e.g. from pools) ‘‘isolating’’ the fluids inside the crater and in the internal chambers. d18O values support a confined seepage of fluids through the feeder channelallowing a bypass through the intervals charged with meteoric fluids.

A. Mazzini et al. / Marine and Petroleum Geology xxx (2008) 1–13 11

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ReferencesBahr, A., Pape, T., Bohrmann, G., Mazzini, A., Haeckel,

M., Reitz, A., Ivanov, M. 2008. Authigenic carbonate precipitates from the NE Black Sea: a mineralogical, geochemical and lipid biomarker study. International Journal of Earth Sciences, DOI. 10.1007/s00531-007-0264-1.

Cronin, B., Çelik, H., Hurst, A., Gul, M., Gürbüz, K., Mazzini, A., Overstolz, M. 2008. Slope-channel Com-plex Fill and Overbank Architecture, Tinker Channel, Kirkgecit Formation, Turkey. In: T.H. Nilsen, R.D. Shew, G.S. Steffens and J.R.J. Studlick (Editors), Atlas of Deep-Water Outcrops. AAPG Studies in Geology, 56, 363-367.

Gisler, G. 2009. Simulations of the explosive eruption of superheated fluids through deformable media. Marine and Petroleum Geology Journal, Special Issue.

Ivanov, M., Blinova, V., Kozlova, E., Westbrook, G., Mazzini, A., Minshull, T. Nouzé, H. 2007. First sam-pling of gas hydrate from the Vøring Plateau. EOS, 88, 209-210.

Mazzini, A., Ivanov, M.K., Nermoen, A., Bahr, A., Borh-mann, G., Svensen, H., Planke, S. 2008. Complex plumbing systems in the near subsurface: geometries of authigenic carbonates from Dolgovskoy Mound (Black Sea) constrained by analogue experiments. Marine & Petroleum Geology, 25, 457-472.

Mazzini A. 2009. Mud Volcanism: Processes and Implica-tions (Editor). Marine and Petroleum Geology Journal, Special Issue (in press).

Mazzini, A., Svensen, H., Akhmanov, G.G., Aloisi, G., Planke, S., Malthe-Sørenssen, A., Istadi, B. 2007. Trig-gering and dynamic evolution of the LUSI mud vol-cano, Indonesia. Earth and Planetary Science Letters, 261, 375-388.

Mazzini, A. Nermoen, M. Krotkiewski, Y. Podladchikov, H. Svensen, S. Planke, 2009. Fault shearing as a mech-anism for overpressure release and trigger for pierce-ment structures. Implications for the Lusi mud volcano, Indonesia. Marine and petroleum Geology (accepted)

Mazzini, A., Svensen, H., Planke, S., Guliyev, I., Akh-manov, G.G., Fallik, T., Banks, D. 2009. When mud volcanoes sleep: Insight from seep geochemistry at the Dashgil mud volcano, Azerbaijan. Marine and Petro-leum Geology, doi:10.1016/j.marpetgeo.2008.11.003.

Skinner Jr, J.A., Mazzini, A. 2009. Martian mud volca-nism: Terrestrial analogies and implications for forma-tional scenarios. Marine and Petroleum Geology (in press).

Svensen, H., Hammer, Ø., Mazzini, A., Onderdonk, N., Polteau, S., Planke, S., Podladchikov, Y. Y. 2009. Dynamics of hydrothermal seeps from the Salton Sea geothermal system (California, USA) constrained by temperature monitoring and time series analysis. Jour-nal of Geophysical Research (in review).

B. Fluid processes

angle of approximately 45� towards the surface. These cracks oftenhave a side-to-side asymmetry, with one crack propagating furtheror faster than the other. The asymmetry is initiated by round-offerror and grows because of stress concentration at the crack tip.Down-propagating cracks start at the surface in these simulations:the surface bows upwards as the diagonal cracks grow, increasingthe tensile stress near the centre until failure occurs.

At higher pressures and higher velocities (to the right and downin Table 1 and Fig. 3), the diagonal cracks are suppressed: they oftenform and then anneal. The behaviour is instead dominated by theformation of a vertical pipe to the surface, tending towards conicalat higher energies (higher pressures or velocities), but straighter atlower energies. The pipe is sometimes accompanied by horizontalopening-mode cracks leading off in either direction, not alwayssymmetrically.

3.1. Run SmtO7: cone sheets?

As an example of diagonal crack development and propagation,we chose to focus on the very nearly symmetrical configurationdeveloped by run SmtO7, which has an injection pressure of0.6 kbar and an injection speed of 500 m/s. Three density snapshotsfrom this run are shown in Fig. 4.

Just 1 s after the start of the calculation (Fig. 4, top), a smallcavity has opened up above the top of the rigid injection pipe. Thesediments immediately above this are crushed to a density of 1.3 g/cc, nearly half solid density, by the static and ram pressure of thefluid exiting the pipe (see inset at top right). Further propagation inthe vertical direction is blocked by jamming, and the fluid seekseasier paths to the side.

After 10 s (middle frame), the diagonal cracks have progressedabout a quarter of the way to the surface, more compaction abovethe pipe has increased the sediment density to 1.6 g/cc. The addedvolume below causes some bowing of the surface 1.7 km above,initiating a downward-propagating crack almost directly above theinjection pipe.

At 20 s (bottom), the diagonal cracks are noticeably, but stillweakly, asymmetric, with the uppermost tip of the right-hand crackonly 400 m below the surface. The downward-propagating crackfrom the centre has reached a depth of 350 m, and smallercracks are evident through much of the volume between thediagonal cracks. At later times (not shown), both diagonal crackspierce the surface, the right one first, and venting occurs. Thecorners of the central triangular sediment block between the cracksare ablated and hurled upward. The triangular block itself first risesand then settles back into the cavity as more downward-

propagating vertical cracks and upward-propagating diagonalcracks form throughout the block. The configuration after 50 s isshown in the appropriate block in Fig. 3.

3.2. Run SmuO7: straight-sided pipe with outburst

A nearly straight-sided vertical pipe is formed in the SmuO7 run,illustrated in Fig. 5, with an injection pressure of 0.8 kbar and speedof 500 m/s. That is, we keep the same injection speed as in theprevious run, but increase the injection pressure.

Once again, the calculation starts off with the ram and staticpressure of the injected fluid producing considerable compactionand therefore jamming immediately ahead of the working surface.Initial crack propagation therefore starts sideways. A compactionwave propagates away from the injection point at the acousticspeed in the sediments (5 km/s). The rarefaction wave returns tothe injection point in just under 1 s, reducing the jamming justenough that the ram pressure can force the opening of a verticalcrack. By 4 s (Fig. 5, top frame), this crack has come towithin 1.2 kmof the surface, and its walls have compacted and hardened toa density of 1.3 g/cc.

At 10 s (Fig. 5, middle frame), a number of diagonal cracks havespawned off the gaping vertical crack, whose tip is now within275 m of the surface. Some downward-propagating cracks havestarted from the surface to meet the big crack. By 25 s (Fig. 5,bottom frame), the crack has relaxed to a narrower width, withfluid streaming vigorously upwards and exploding outwardsthrough the funnel-like crater. A significant amount of fragmentedsedimentary material is entrained in the flow, both as large chunksand fines.

In an animation of this simulation, the vent is seen to openviolently at about 12 s, with significant erosion and entrainment ofmaterial from near the opening. This is illustrated in Fig. 6, ina sequence of six frames from the animation, showing just thebreakout region, from 11.5 s to 15.5 s.

3.3. Run SmuO4: conical pipe with geyser

In run SmuO4 (see Fig. 7), we increase the injection speed to1500 m/s and keep the injection pressure at 0.8 kbar. This runresults in a pipe that is more conical, and a crater resembling thebell of a trumpet.

In this case the ram pressure due to the high injection speedoverwhelms jamming above the injection, and compaction occurson the sides of the vertical pipe. There is therefore no significanttendency towards sideways crack propagation until after the strong

Fig. 6. Log density raster images from the central portion of the run shown in Fig. 5 (Smu07), shown at intervals of 1 s, from 11.5 s through 16.5 s. The violence of the breakout ripsmaterial from the surface adjacent to the opening and entrains it into the flow.

G. Gisler / Marine and Petroleum Geology xxx (2009) 1–86

ARTICLE IN PRESS

Please cite this article in press as: Gisler, G., Simulations of the explosive eruption of superheated fluids through deformable media, Marine andPetroleum Geology (2009), doi:10.1016/j.marpetgeo.2008.12.006

Figgure B8 Simulation with the Sage code of the eruption of high pressure fluids through a deformable medium, representing a sedimentary basin. This image shows a sequence at intervals of 1 second, in a calculation in which a pipe is formed by the rapid release of supercritical fluid from a reservoir at depth, and then erupts, geyser-like, at the surface. The colour scale is logarithmic in the density, and vectors show the fluid flow. Cracks form in the deformable medium and then anneal as the medium’s strength is insufficient to hold them open against the dynamic pressure of the released volatiles.


Central Scientific ProblemMagmatic intrusions in sedimentary basins often form hori-zontal sills and frequently exhibit saucer-shaped morpholo-gies. They are of significant economic interest because they af-fect oil maturation and migration pathways, form traps for pe-troleum and sometimes act as water reservoirs. They are often associated with large igneous provinces and climate change, so they are also of high scientific importance.

Figure B9 (A) Aerial view of the Golden Valley Sill. (B) Geological map of the Golden Valley Sill Complex showing the location of sampling sites (in general, one point corresponds to both opposite sill margins). X and Y axes are longitude and latitude in degrees. (C) Simplified geological cross section of the Golden Valley Sill Complex. (D) Schematic profile of the Karoo Basin region showing simplified stratigraphy and intrusive complex.

Recent ResultsMagmatic sill intrusions tend to develop saucer-like geome-tries in layered sedimentary basins intruded by large volumes of magma. The Karoo Basin of South Africa hosts hundreds of saucer-shaped sills. Among these, the Golden Valley Sill (Figure B9) is well exposed and displays connections with ad-jacent and nested saucers. Previous models for the emplace-ment of such saucer-shaped sills have usually been based on analysis of the intrusion geometry and the spatial relationships with potential feeders, rather than on magma flow patterns.

Stephane Polteau (Pol-teau et al 2008) and co-workers, using de-tailed field observations and magnetic suscep-tibility measurements, were able to infer flow directions, and thereby place constraints on the emplacement mecha-nism. The data support a model consisting of a point feeder supplying magma in a radial pat-tern to form the saucer-shaped sill, rather than feeding by dikes.

3. Sill emplacement

which are collectively referred to as the Golden Valley SillComplex (Figures 1b and 1c). The Golden Valley SillComplex intruded the Karoo subhorizontal sedimentarystrata of the upper Permian – Lower Triassic Beaufort Groupat 1 to 2.4 km depth (Figure 1d) [Polteau et al., 2008].[5] An individual saucer-shaped sill can be divided into

three morphological parts, a subhorizontal inner sill formingthe base, dikes referred as steeply dipping inclined sheetscrosscutting the subhorizontal sedimentary strata and asubhorizontal outer sill [Chevallier and Woodford, 1999].The inclined sheets commonly dip inward at 20–65� andclimb 100–300m to connect the lower inner sill with theupper outer sill [Chevallier and Woodford, 1999]. Minorsills are secondary sills that may be present within a saucer-shaped intrusion [Chevallier and Woodford, 1999].

2.2. New Field Observations

[6] The nature of the contact separating two superposedsills is of primary significance when looking at the emplace-

ment mechanism of a sill complex. In the Golden ValleySill Complex, two superposed sills are either separated bychilled margins or by a �50 cm thick baked shale layer(Figures 2a, 2b, and 2c). We have not observed themerging of two superposed sills or the frontal terminationlobe of a dolerite sheet.[7] A 1 m thick horizontal minor sill outcrops in the

southern portion of the Golden Valley, approximately 2 mabove the inner sill. Eight ropy flow structures [Liss et al.,2002] are present on the upper surface of the minor sill. Allthe ropy flow structures are elongated vesicles trendingN220� (Figure 2d).[8] The inclined sheets locally exhibit 50 m wavelength

undulations of their upper surface, a feature observed in 3-Dseismic interpretations [Thomson and Hutton, 2004]. Theundulations form tubular geometries defined by the size ofthe columnar jointing, about 4m wide hexagonal columnsalong the crests and only 2m wide columns along thetroughs (Figure 2e). The axes of these undulations dip

Figure 1. (a) Aerial view of the Golden Valley Sill. (b) Geological map of the Golden Valley SillComplex showing the location of sampling sites (in general, one point corresponds to both opposite sillmargins). X and Y axes are longitude and latitude in degrees. (c) Simplified geological cross section ofthe Golden Valley Sill Complex. (d) Schematic profile of the Karoo Basin region showing simplifiedstratigraphy and intrusive complex.

B12104 POLTEAU ET AL.: HOW ARE SAUCER-SHAPED SILLS EMPLACED?

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B12104

B. Fluid processes


Figure B10 The Waterdown Dam locality in South Africa’s Karoo Basin. (A) Overview of the locality, showing a transgressive dolerite sill and the road cut along R67 with sediment dike localities. (B) Sediment dikes along the road cut that can be traced 10-15 vertical meters. (C) A 2 meter thick breccia dike within the dolerite. (D) Close-up of the dike in frame C, showing a dolerite fragment within the baked sandstone. Note the irregular fragment in the lower right, possibly representing altered magmatic material. Coin for scale. (E) Close-up of a sediment dike showing sediment fragments and the dolerite “bridge” extending from the walls and into the dike. Hammer for scale.

B. Fluid processes


B. Fluid processes

Figure B11 Schematic model of aureole processes. A. Sketch of a magmatic sill that has intruded into a sedimentary basin. The rock immediately adjacent to the sill, transformed by the heat of the magma, is known as the aureole. Sometimes vent complexes arise from the ends of sills and penetrate all the way to the surface. B. Close-up of a portion of the sill and aureole, illustrating the release of water molecules from minerals and the release of methane from kerogen during contact metamorphic processes.

Sediment injections within dolerite sills are common in the Karoo Basin. These have been the subject of investigations by Ingrid Aarnes and co-workers (Aarnes et al 2008, Svensen et al 2009). Numerical modeling and field investigations have shown that the sediment dikes were intruded into the sills when the sills had cooled sufficiently to reduce their internal pressure relative to the pressure in the surrounding aureole, but while still hot enough to produce the observed contact metamorphism seen within the dikes (Figure B10). The dikes were thus sucked into cracks within the cooling and contract-ing sills.

Contact aureoles in sedimentary basins around magmatic sills may play important roles in past episodes of climate change (Aarnes et al 2008). Contact metamorphism of the sediments in the aureoles, heated by the intruding magma, leads to the production of fluids and gases that seep out into the surround-ing medium and in some cases produce vent complexes direct-ly leaking these volatiles into the atmosphere (Figure B11).

ReferencesAarnes, I., Podladchikov, Y.Y., Neumann, E-R. 2008.

Post-emplacement melt flow induced by thermal stresses: Implications for differentiation in sills, Earth and Planetary Science Letters, 276, 152-166.

Aarnes, I., Svensen, H., Polteau, S. 2008. Gas formation from black shale during contact metamorphism: Con-straints from geochemistry and kinetic modeling, LASI III Conference.

Aarnes, I., Svensen, H., Connolly, J.A.D., Podladchikov, Y.Y. 2009. Modeling of contact metamorphism in shales and the implications for gas generation in sedimentary basins. (In prep.).

Galland, O., Cobbold, P. R., Hallot, E., de Bremond d’Ars, J. 2008. Magma-controlled tectonics in com-pressional settings: insights from geological examples and experimental modelling, Bollettino Della Società Geologica Italiana (In press).

Polteau, S., Mazzini, A., Galland, O., Planke, S., Malthe-Sørenssen, A. 2008. Saucer-shaped intrusions: Oc-currences, emplacement and implications. Earth and Planetary Science Letters, 266, 195-204.

Polteau, S., Ferré, E.C., Planke, S., Neumann, E.-R., Chevallier, L. 2008. How are saucer-shaped sills em-placed? Constraints from the Golden Valley Sill, South Africa. Journal of Geophysical Research, 113, B12104, doi:10.1029/2008JB005620.

Svensen, H., Aarnes, I., Podladchikov, Y.Y., Jettestuen, E., Harstad, C.H., Planke, S. 2009. Sandstone dikes in dolerite sills: Evidence for high pressure gradients and sediment mobilization during solidification of magmatic sheet intrusions in sedimentary basins, Geopsphere, (Subm.).


B. Fluid processes

Figure B12. Shallow seismic reflection studies of the Oslofjord pockmarks.

4. Fluids and Sediments: Travertines and Pockmarks

Central Scientific ProblemThe precipitation of suspended sediment from fluids in motion, and the ablation and suspension of sediments removed from topographic irregularities, shape patterns that occur world-wide in earth’s crust, including travertine terraces surround-ing mineral-bearing springs and pockmarks on the seafloor. The physics of fluids, reactive chemistry and interaction with granular material are key to understanding these processes.

Recent ResultsTravertine terracing is one of the most eye-catching phenom-ena in limestone caves and around hydrothermal springs, but remains fairly poorly understood. The interactions between water chemistry, precipitation kinetics, topography, hydrody-namics, carbon dioxide degassing, biology, erosion and sedi-mentation constitute a complex, dynamic pattern-formation process. The processes can be described and modeled at a range of abstraction levels. At the detailed level concerning the physical and chemical mechanisms responsible for pre-cipitation localization at rims, a single explanation is probably insufficient. Instead, a multitude of effects are likely to con-tribute, of varying importance depending on scale, flux and other parameters.

A three-year “YFF” project funded by NFR and led by Øyvind Hammer on the geology and biology of springs and pock-marks came to an end in 2008. This project has focused on pockmarks (large underwater craters) in the Oslofjord and the Norwegian Sea. The team have collected large amounts of information on the geology (Figure B12) and biology of these enigmatic structures. Detailed studies of cores and seismic data have led to a good understanding of the history (if not the process) of the Oslofjord pockmarks, showing that they initially formed during the end-Pleistocene deglaciation but have been kept open since then. New data indicate that those in the Oslofjord probably formed by seepage of fresh ground-water, though present expulsion of gas or fluids has not been detected. Pockmarks in the Norwegian Sea have been found to have high biological abundance and diversity (Figure B13), while those of the Oslofjord are less diverse. A new theory for the survival of pockmarks through long periods of time by current activity has been tested by supercomputer simulation (Figure B14) and field studies. New statistical methods have been developed as part of the work.


B. Fluid processes

Figure B13. Biological communities and carbonate rocks from the Troll pockmarks in the Norwegian Sea. A) East slope with abundance of anemones. B - D) Heavily encrusted carbonated rocks E) Gorgonian coral, Paragorgia arborea. F) Centre of pockmark with the Gorgonian coral, Paragorgia arborea, and the bivalve, Acesta excavate.


B. Fluid processes

Figure B14. Cross-section of a three-dimensional simulation of undersea currents deflected by a seafloor pockmark.

ReferencesAkhmetzhanov, A.M., Kenyon, N.H., Ivanov, M.K.,

Westbrook, G. Mazzini, A. 2008. (Editors). Deep-water depositional systems and cold seeps of the Western Mediterranean, Gulf of Cadiz and Norwegian continen-tal margins. IOC Technical Series No. 76, UNESCO, 91 pp.

Hammer, Ø. 2008. Pattern formation: Watch your step. Nature Physics, 4, 265-266.

Hammer, Ø., Dysthe, D.K., Lelu, B., Lund, H., Meakin, P. , Jamtveit, B. 2008. Calcite precipitation instabil-ity under laminar, open-channel flow. Geochimica et Cosmochimica Acta, 72, 5009-5021.

Hammer, Ø., Dysthe, D.K., Jamtveit, B. Travertine terracing: patterns and mechanisms. In: Tufas and Speleothems: Unravelling the Microbial and Physical Controls. Geological Society of London Special Publi-cations (Accepted).

Hammer, Ø., Webb, K.E., Depreiter, D. Upwelling cur-rents in pockmarks. Geo-Marine Letters (In review).

Hammer, Ø. New statistical methods for detecting point alignments. Computers & Geosciences, 35, 659-666.

Webb, K.E., Hammer, Ø, Lepland, A. & Gray, J.S. Pock-marks in the Inner Oslofjord, Norway. Geo-Marine Letters (In press, released on-line).

Webb, K.E., Barnes, D.K.A., Planke, S. Pockmarks: refuges for marine benthic biodiversity? Limnology and Oceanography (In veriew).

Webb, K.E., Barnes, D.K.A., Gray, J.S. Benthic ecology of pockmarks and the Inner Oslofjord, Norway. Marine Ecology Progress Series (In review).


B. Fluid processes

5. Violent processes

Central Scientific ProblemMany of the processes that produce large-scale patterns in the Earth’s crust are violent; especially those that produce our planet’s most striking and beautiful landscapes. Fortunately, violent events are relatively infrequent, but a significant frac-tion of Earth’s human population lives in areas that are highly vulnerable. The 200,000 human lives lost in the Indonesian earthquake and tsunami in December 2004, or the 80,000 lost in the Pakistan earthquake in October 2005 give us a com-pelling moral interest in understanding these events with the ultimate goal of protecting and saving human lives.

Recent ResultsThe multi-material adaptive-mesh hydrocode Sage (from Los Alamos and Science Applications International) has been ap-plied to an increasing variety of violent processes in geophys-ics, including asteroid impacts, mud volcanism, and landslide-driven tsunamis.

In 2008, Galen Gisler made further studies of asteroid impact models, examining the distribution of ejecta from oblique im-pacts with particular application to the Chicxulub impact at the end of the Cretaceous Period (Gisler et al. 2009) Steeper impacts make larger craters and more symmetrical ejecta dis-tributions, although butterfly patterns persist up to 60-degree inclinations. Appreciable amounts of material can be moved great distances without suffering high pressures or tempera-tures simply by being carried along by the bulk motion. The ongoing application of similar models to other shallow-water impacts like the Mjølnir crater and the Gardnos crate show that vast quantities of sediment can be transported by many kilometres in such events, making the crater morphology hard to interpret (Gisler and Tsikalas, in preparation, see Figure B15). The amount of water covering an impact site makes a very significant difference in the crater that is produced. In shallow, or no water, the effects of impact are strongly loca-lised, but large quantities of water tend to spread out the ef-fects, making the damage less intense locally but more wide-spread. In very deep water, as in ocean basins, craters do not occur at all unless the impactor diameter is comparable to the ocean depth.

Figure B15 Sediment transport in the Mjølnir crater, modeled as the impact of a 1 km asteroid into 500 m water covering 3 km of unconsolidated sediment above a thick carbonate platform. Coloured lines represent the positions of Lagrangian massless tracer particles as a function of time from their initial positions (red) to their positions after 3 minutes (violet). Most particles, except those very near the centre at the beginning, move several kilometers closer to the crater centre. The background grey scale is a density plot showing the crater configuration at 3 minutes after impact.


B. Fluid processes

Tsunamis from submarine and subaerial landslides are also a major focus of the violent processes work. Since the rheology of the slide material has been shown (Gisler 2008, see Figure B16) to be a major factor in the characteristics of the resulting tsunami, it is desirable to pin down the properties of the slides more closely. In consultation with researchers at the National Oceanographic Centre in Southampton, Gisler has begun a study of the El Golfo slide off the island of Tenerife in the Ca-naries. This slide, which occurred some 8000 years ago, has a runout of 65 km and is very smooth. In a series of simulations which are still continuing, we have learned that the runout distance and the smoothness put important constraints on the rheology: too runny, and the slide breaks up into turbidity cur-rents; too viscous, and the slide stops too early. High numeri-cal resolution is important for treating this problem, so this work continues. The implications of this study will have bear-ing on the potential danger posed by the possibility of a major landslide in the future from the island of La Palma (Løvholt et al 2008).

ReferencesGisler, G.R. 2008. Tsunami simulations, Annual Review

of Fluid Mechanics, 40, 71-90.Gisler, G.R. 2009. Tsunami generation - other sources,

chapter 6 in The Sea: Volume 15, Tsunamis, edited by Alan Robinson and Eddie Bernard, pp 179-200.

Gisler, G.R., Weaver, R.P., Gittings, M.L. 2009. Oblique impacts into volatile sediments: ejection distribution patterns, PARA 08 Conference Proceedings, Trond-heim. (In press).

Løvholt, F., Pedersen, G.K., Gisler, G.R. 2008. Oceanic propagation of a potential tsunami from the La Palma Island, Journal of Geophysical Research, 113,C09026, doi:10.1029/2007JC004603.

Figure B16 Simulations of landslides with varying material properties into an ocean. When the material is stiff, the runout is shorter, and the relict on the seafloor is smoother. Very runny material produces long runouts but leave relicts that are bumpy. These snapshots are from five different runs with different rheologies, all at a time of 300 seconds after the start of the landslide. The underlying topography is that of the El Golfo slide off Tenerife in the Canaries, which has an observed runout of 65 km and is very smooth. None of these models match, since the simulated slides have already decelerated significantly by the time these snapshots are taken.


Our research on the dynamics of deformation localisation in the earth encompasses the brittle, transitional and ductile deformation regimes, concentrating on meso-scale phenom-ena. The dynamics of microstructures and interface processes strongly influence how, where and when localisation occurs as well as its persistence in different environments. Similarly, localization processes themselves will influence subsequent mechanical behaviour and hence dynamic processes operat-ing on a geodynamic scale.

We are continuing a multi-faceted approach to individual yet complementary projects and below we present three current research projects: Force chains in granular systems; Non-hydrostatic compaction and decompaction; and Hierarchical fracturing during serpentinisation.

1. Pore-scale inelasticity and seismic wave attentuation in reservoirsIntroduction

Scientific problemIn this study, we revisit the idea that micro-scale yielding is responsible for attenuation of seismic waves over a wide frequency range. Hydrocarbon-saturated zones often show anomalously high attenuation, from measurements of quality factor (Q). Q is considered to be frequency dependent over a wide frequency band, but in dry rock, over limited frequency ranges, Q is essentially frequency independent. The combined observations of frequency independent Q, and the established role of microcracks on attenuation, have been interpreted in terms of frictional sliding at grain boundaries or across crack faces. However, for typical strain amplitudes of seismic waves and reasonable microcrack dimensions the computed slip across crack faces was negligible. In addition, frictional at-tenuation results in nonlinear wave propagation, while early available data showed that at low strains typical of seismic waves (<10-6) the rocks behaved linearly. It was therefore con-cluded that such a nonlinear mechanism was not relevant for seismic waves. Recent observations, however, show the pres-ence of nonlinear effects in rocks at strains as small as 10-9. The permanent and, importantly, time independent (plastic) deformation in rocks at typical seismic strains was explicitly observed in laboratory experiments. Plastic yielding would not be expected in a stress-free rock sample loaded by small seis-mic strains, however, sediments may be at or close to a yield state as a result of complex burial and tectonic loading history. Moreover, rocks are highly heterogeneous and heterogeneities may act as local stress concentrators, so that the actual micro-scopic stresses around cavities and inclusions may be much higher than the macroscopic stress level.

C. Localisation processes

Figure C1 Pseudotachylyte injection vein in peridotite Corsica. Vein is formed by near 100% melting along seismic fault in the mantle peridotite during the Alpine orogeny. Notice dilation during injection of the vein.


Figure C2 Model of a representative volume element of porous media.

Figure C3 Model predictions and data collapse for quality factor Q

1. Pore-scale inelasticity and seismic wave attentuation in reservoirs

Approach and resultsWe study attenuation of seismic P- and S-waves due to local plastic yielding around cavities in porous media. Following the effective media approach, we consider low po-rosity material containing non-interacting isolated spherical or cylindrical pores under cyclic loading by both isotropic and shear stress field, imitating the passage of a wave, and evalu-ate resulting dissipation in terms of quality factor Q. Assuming initial local microscopic stress state around the cavity at the yield, we show that even for small seismic strains, attenua-tion can be high and independent of both frequency and strain amplitude.

ReferencesYarushina V.M., Podladchikov Y.Y. “Low-frequency

attenuation due to pore-scale inelasticity”, Geophysics, (in review).

Yarushina, V.M., Podladchikov, Y.Y. 2008. “Microscale yielding as mechanism for low-frequency intrinsic seis-mic wave attenuation”, Conference proceedings, 70th EAGE Conference & Exhibition — Rome, Italy, 9 - 12 June.



Scientific problemStrain localization has important implications for the mechan-ical strength and stability of evolving fault zones. Structural fabrics interpreted as strain localization textures are com-mon in natural and laboratory faults, however, the dynamic microscale processes controlling localization (and delocaliza-tion) are difficult to observe directly. Discrete numerical mod-els of faulting allow a degree of dynamic visualization at the grain scale not easily afforded in nature. When combined with laboratory validation experiments and field observations, they become a powerful tool for investigating the dynamics of fault zone evolution.

Approach and resultsWe present a method that implements realistic gouge evolu-tion in 3D simulations of granular shear. The particle-based model includes breakable bonds between individual particles allowing fracture of aggregate grains that are composed of many bonded particles. During faulting simulations, particle motions and interactions as well as the mechanical behavior of the entire system are continuously monitored. We show that a model fault gouge initially characterized by mono-dis-perse spherical aggregate grains gradually evolves, with accu-mulated strain, to a wide size distribution. The comminution process yields a highly heterogeneous textural signature that is quantitatively comparable to natural and laboratory produced fault gouges. Mechanical behavior is comparable to a first order with relevant laboratory data. Simulations also reveal a strong correlation between regions of enhanced grain size reduction and localized strain. Thus in addition to producing realistic fault gouge textures, the model offers the possibility to explore direct links between strain partitioning and structural development in fault zones. This could permit investigation of subtle interactions between high and low strain regions that may trigger localization - delocalization events and therefore control macroscopic frictional stability and hence the seismic potential of evolving fault zones.

2. Fragmentation and strain partitioning in faults


In addition to the projects described above, work is ongoing in: localization and shear heating; laboratory investigation of aftershocks; thermal imaging and roughness development of faults.

ReferencesAndersen, T.B., Mair, K., Austrheim, H., Podladchikov,

Y.Y., Vrijmoed, J.C. 2008. Stress-release in exhumed intermediate-deep earthquakes determined from ultra-mafic pseudotachylyte. Geology, 36, 995-998.

Bjørk, T.E., Mair, K., and Austrheim H. 2009. Quantify-ing fault rocks and deformation: advantages of combin-ing grain size, shape and phase differentiation. Journal of Structural Geology, (in press).

Sarwar, M. 2008. Energy dissipation in a simulated fault system, Masters thesis, PGP, University of Oslo.

Mair, K., Abe, S. 2008. 3D numerical simulations of fault gouge evolution during shear: Grain size reduction and strain localization. Earth and Planetary Science Letters, 274, 72-81.

Forskningsradet eVITA Magazine article on Mair and Abe fault modelling work: Nytt fra eVITA, Nr2, November 2008 ‘Stanser jordskjelv midt i utviklingen’ (‘Stopping an earthquake in its midst’)


Figure C4 3D DEM Model of fault showing initial (top) and final (bottom) configuration after 200% shear strain. Model contains ~190.000 particles. The particles in both images are colored according to their aggregate ‘parent’ grain.

Figure C5. Spatial distribution of matrix fraction after 200% shear strain is plotted on a 2D slice of the 3D model. We see local zones of high matrix content (yellow) i.e. enhanced grain size reduction close to the upper and lower fault zone boundaries and regions of low matrix content (blue) i.e. survivor grains inside.




ReferencesVrijmoed, J.C., Smith, D.C., van Roermund, H.L.M. 2008.

Raman confirmation of microdiamond in the Svartber-get Fe-Ti type garnet peridotite, Western Gneiss Region, Western Norway. Terra Nova, 20, 295-301.

Vrijmoed, J.C., Podladchikov, Y.Y., Andersen, T.B. An alternative model for ultra-high pressure in the Svart-berget Fe-Ti garnet-peridotite, Western Gneiss Region, Norway. European Journal of Mineralogy, (in press).

Vrijmoed, J.C. Pressure variations during ultra-high pres-sure metamorphism from single grain to outcrop scale? Journal of Metamorphic Geology (soon to be submit-ted).

Vrijmoed, J.C., Austrheim, H., John, T., Davies, G.R., Corfu, F. Metasomatism of the ultra-high pressure Svartberget Fe-Ti type garnet-peridotite, Western Gneiss Region. Norway. Journal of Petrology, (soon to be sub-mitted)..

Scientific problemUltra-high pressure (UHP) rocks, recording mantle-like pres-sures (3.0 - 5.5 GPa) but hosted by mid-crustal (much lower pressure) rocks are difficult to explain, particularly in conti-nental collision orogens where no evidence for deep burial (to UHP conditions) or extreme exhumation (from UHP con-ditions) exists. At Svartberget (W. Norway), a peridotite en-clave in mid-crustal felsic migmatitic gneiss is exposed. The enclave is crosscut by vein filled fractures showing evidence for melt reactions and containing microdiamond (Figure C6a). Peak P-T estimates for these veins (5.5GPa, 800 ºC) would suggest burial depth exceeding 150 km. However, although field structural evidence supports exhumation from normal HP-UHP conditions (2.5-3GPa), no evidence exists to explain exhumation from the extreme UHP conditions (5.5 GPa) ob-served. In addition it is difficult to explain: i) Deformation of the rheologically strong peridotitic rocks (forming brittle frac-tures filled with UHP veins), and ii) Melt reactions along the fractures (Figure C6b) in the peridotite where temperatures are well below the melting temperature of peridotite.

Approach and resultsWe have conducted an interdisciplinary study including de-tailed field mapping, petrography, mineral-chemistry, whole rock (isotope) geochemistry, dating and numerical model-ling to provide a possible explanation for these observations. In our conceptual model, localised melting of gneisses in the mid-crust and associated volume expansion leads to Ul-tra High Pressures. Pore fluid pressure builds up due to the melting and significantly weakens the peridotitic rocks at the boundary between gneiss and peridotite, leading to the brit-tle failure of these strong rocks. High pressure reactive melts from the gneiss then infiltrate the peridotite and react to form diamond bearing websterite veins. Eventually the surrounding lithosphere will also fracture thereby releasing the overpres-sure. Our numerical model, focussing on the pressure build up stage, indicates that pressure build, by localised melting of felsic gneiss, could reach several GPa (high enough to form diamond) and that an irregularly shaped inclusion of rheologi-cally strong rock, such as peridotite, could give rise to differ-ential stresses that may explain the conjugate set of fractures observed in the Svartberget peridotite.

3. Ultra-high pressure rocks



Figure C6 a) Simplified geological map of the Svartberget peridotite. The whole body (olive-green) is cut by a conjugate set of fractures along which melt reactions took place leading to the formation of diamond bearing phl-grt-websterite (dark green) and garnetite (red) veins. (Grey colours indicate other rock types). b)Close up of the area (a) showing details of the veins. c) Result of elastic FEM calculation showing the overpressure resulting from localised melting of gneisses in the mid-crust. The outer part (mainly blue) represents the non-molten rocks of the lithosphere, surrounding a ring (mainly red) of gneiss (represented as white on map 1a) that is 10x weaker and that expands due to formation of a lower density melt. In the middle an enclave with the same rheology as the non-molten rocks represents the peridotite. Note how the shape of the peridotite gives rise to a heterogeneous pressure field (slightly different red colours) corresponding to the development of differential stresses. This situation would arise after 100ºC in temperature corresponding to 50% melting.

0 5 102.5 m-

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(a) (b)

(b)

felsic migmatitic gneiss

P (GPa)

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Introduction

IntroductionThe main focus of the microstructures group in 2008 has been the study of the deformation of heterogeneous and/or aniso-tropic materials, the coupling to reactions, and the develop-ment of efficient numerical models. First an overview over last year’s published papers is given and then two active research topics are discussed in detail. Our research on the deformation of layered media has yielded four papers. In Schmid et al., (2008) have we demonstrated the capabilities of our BILAMIN code. BILAMIN is an unstruc-tured (body fitted) finite element method (FEM) code that is capable of solving problems with more than 100’000’000 de-grees of freedom in three dimensions (described in the 2007 PGP Annual Report). The paper was published in a special volume of “Physics of the Earth and Planetary Interiors” en-titled “Recent Advances in Computational Geodynamics: Theory, Numerics and Applications” and BILAMIN clearly stands out in terms of state of the art computing in earth sci-ences. The second paper on folding is by Jäger et al. (2008) entitled “Brittle fracture during folding of rocks: A finite ele-ment study”. It deals with the frequently encountered problem of simultaneous ductile and brittle deformation, which usually represents a problem for continuum based approaches such as FEM. The problem can be solved with the extended finite element method. However, the extension to large strain, three dimensions, and multiple crack propagation make this a tech-nically challenging problem. The third paper on the deforma-tion of layered material is by Schmalholz et al. (2008) and deals with boudinage in power-law materials. Analytical and FEM models are used to analyse this necking instability and to quantify under which conditions it occurs and what informa-tion can be extracted from natural pinch and swell structures. A fourth paper in this series was published by Marques and Podladchikov (2009) who demonstrate the importance of a strong elastic layer for the fold pattern formation on the large scale.

D. Microstructures

After some trouble with publishing our concept of “mechani-cal closure” we finally succeeded and two papers now docu-ment our experiments and the corresponding theory regarding enstatite rim growth in mixtures of quartz and olivine: Milke et al. (2009) and Schmid et al. (2009). Another paper in the context of coronas is by Austrheim et al. (2008) who found that micro zircons in gabbros often form a three dimensional framework, which traces former grain boundaries. Therefore these zircon networks can be used to a) document the previ-ous presence of minerals, b) quantify the element transport, and c) gain information on the mechanism of metamorphic and metasomatic processes. Micro zircon networks seem to be quite common in natural rocks and therefore this novel concept developed by Austrheim et al. widely applicable.

The behavior of particle suspension systems is an active re-search topic at PGP. In the following we present two relevant research projects. First we introduce a study on how deforming particle suspension systems can be solved efficiently in three dimensions on a single desktop computer by using Stokesian dynamics, an approach that was implemented by Espen Jettes-tuen. In a second study we demonstrate how rocks become mechanically anisotropic as they deform. Most natural rocks exhibit some form of mechanical anisotropy, either they are explicitly layered, or the constituents are preferentially aligned, or the different phases exhibit internal (lattice preferred orien-tation) anisotropy. Nevertheless, mechanical material anisot-ropy is usually ignored in structural geological and tectonic models, often due to theoretical or numerical complications. Marcin Dabrowski has studied the role of mechanical anisot-ropy as part of his PhD thesis at PGP (Dabrowski, 2008). The study that is presented in the following is an excerpt from his thesis’ paper 3 and provides an improved estimate for the ef-fective anisotropic material properties of deforming heteroge-neous materials.


OverviewThe models run in the microstructures group are usually based on codes that employ body fitting finite element method codes, e.g. MILAMIN (Dabrowski et al., 2008) and BILAMIN (Schmid et al., 2008). This approach yields the most accurate results as the computational grids and the material boundaries coincide. Unfortunately, it is also the computationally most intense method and for three dimensional problems access to large clusters is required for long time periods. Another ap-proach is to give up on the body fitting mesh requirement and to use regular grids. Introducing operator splitting the com-plexity of the three dimensional model can be further reduced to essentially one dimensional problems; a direction that is pursued in Krotkiewski et al. (2008).

A viable alternative for the study of three dimensional particle suspensions systems under the influence of body or external forces are Stokesian dynamics (SD). The SD method was de-veloped in the 80s by Brady and Bossis (1988) and essentially solves the full three dimensional problem by reducing it to the particle characteristics, which can be solved analytically. Thus the inter particle fluid is only visible as a coupling pa-rameter. This simplification is possible due to the linearity of the Stokes equations. The system is translated into a system of linear equations relating the dynamical quantities of the par-ticles (like velocities and spins) to the mechanical quantities (like forces and torques).

The development of SD codes is relatively complex due to the following reasons. 1) If particles get close to each other or near walls special treatment is required because the dilute as-sumption of underlying analytical solutions becomes invalid. 2) Since the individual particle problem has to be solvable analytically the particle geometries have to be simple, prefer-entially spherical. 3) The calculation of the coupling constants between particles is related to the multipole expansion, which is, simply put, an expansion where the small parameter is the inverse of length. This expansion converges fast for dilute sus-pensions, where inter particle distances are long, whereas the convergence is slow for concentrated particle suspensions.

Thus most of the computational research in SD is focused on either finding fast methods to calculate the expansions or to work around them by, for example, adding exact two particle solutions for nearly touching particles. 4) The resulting linear equation systems exhibit full matrices, which makes the solu-tion for large numbers of particles (>10’000) difficult because of memory and CPU requirements.

The advantages of the Stokesian dynamics approach are obvi-ous by looking at the characteristics of the corresponding PGP code: StokesDyn. StokesDyn runs on a standard desktop com-puter and can solve systems with thousands of particles up to large strains within a day. The involved particles are truly rig-id, which in corresponding FEM calculations requires special treatment. StokesDyn can be applied to gravity driven flow, see Figure 1, as well as boundary driven flows such as pure and simple shear. The Stokesian dynamics approach comple-ments the FEM calculations. StokesDyn allows us to quickly explore a wide range of parameters and to obtain an overview of the behavior of the studied system. FEM can then be used to calculate specific configurations and to investigate effects that cannot be analyzed with StokesDyn such as non-linear rheologies and complicated particle shapes. Visualization

The visualization of scientific result s is a challenging task, es-pecially three dimensional ones such as produced by Stokes-Dyn. Here we usually employ ParaView, an open source scientific visualization package that can deal with extremely large datasets using distributed memory computing resources (www.paraview.org). However, given the progress in computer generated imagery in, for example, movie special effects and video games we set out to investigate the possibility to render scientific results with state of the art ray tracing technology.

D. Microstructures

1. Stokesian Dynamics


Figure D1 shows the result of a Stokesian dynamics calcula-tion that is visualized with the free rendering engine POV-Ray (www.povray.org). In the initial configuration the light glass balls are at the bottom and the heavier golden balls at the top, the matrix has an intermediate density. Both types of spheres are assumed rigid. Once gravity is activated the un-stable configuration causes the glass spheres to rise and the golden spheres to sink. Due to the dense packing, spheres can get temporarily trapped and moved in the “wrong” direction, a

model that allows, for example, studying the mixing processes in crystallizing magma chambers. The features of POV-Ray, e.g. several kinds of light sources, reflections, refraction, and light caustics, allow for photorealistic scene rendering. How-ever, it seems that because we are trained to perceive scientific results in abstract illustrations the photorealistic result visual-ization almost gives a “non-scientific” impression. However, photorealistic result rendering can be used in a complemen-tary fashion in scientific visualization.

Figure D1 Visualization of a Stokesian dynamics result.

D. Microstructures


Anisotropic DEMIn the two dimensional anisotropic DEM, the medium is con-structed in an iterative manner by placing a given area fraction of aligned individual inclusions of aspect ratio into the host and reevaluating the host properties after each iteration step. Both, inclusion and host phase are isotropic and the in-clusion host viscosity ratio is . The effective nor-mal and shear viscosities are obtained by integrating two coupled ordinary differential equations

where

The initial values of and are 1.

Using finite element modeling allows us to directly resolve the anisotropic mechanical response of composites consisting of aligned inclusions. We systematically scan through the pa-rameter space of inclusion concentration (up to 50%), aspect ratio (up to 16) and viscosity ratio (between 1/1000 to 1000). Selected results are shown in Figure D2. The DEM estimate proves to provide a very good fit to the numerical results. In particular, it is capable of differentiating models with strong and weak load bearing phase. It also predicts bounded results at high concentrations and large viscosity ratios.

D. Microstructures

2. Mechanical Anisotropy Development of a Two-Phase Composite Subject to Large Deformation

The overall mechanical response of a heterogeneous rock may become anisotropic due to the development of shape preferred orientation (SPO). Laminated materials exhibit a maximal de-gree of anisotropy, where shear and normal viscosities assume values corresponding to the lower (Reuss) and upper (Voigt) theoretical bounds. However, the model of a laminate is not suitable for studying the transient stage of the anisotropy evo-lution during the SPO build up, such as depicted in Figure D3. A major improvement is the anisotropic self consistent aver-aging (SCA) model developed by Fletcher (2004) that incor-porates the effects of finite SPO magnitude and is free of any phenomenological fitting parameters. The SCA scheme is not optimal for composites with distinct inclusion-host geometry at high concentrations and large viscosity ratios. For example, it is insensitive to interchanging the weak and strong phase at 50% concentration. For circular inclusions, the SCA prediction is just a geometrical mean of the inclusion and host viscosi-ties irrespective of whether a strong or weak phase forms the load-bearing host. Thus, the effective viscosity is not bounded when the concentration of a rigid phase exceeds 50%. Yet, the percolation and rheological thresholds are expected to occur at higher inclusion concentrations.

In this work, we develop an anisotropic differential effective medium (DEM) scheme that is better suited for the studied composite type (inclusions-host systems) than SCA. The ef-fective anisotropic viscosity is numerically evaluated for a wide class of inclusion-host models to validate the different effective medium approaches. Finally, the anisotropic DEM scheme is employed to study the anisotropy development in a heterogeneous medium subject to large deformation.

f a b

Figure D2 Effective normal (n) and shear (s) viscosity for composites consisting of 256 non-overlapping, randomly located, aligned elliptical inclusions. Vertical bars show the FEM result span for 10 different inclusion configurations. Upper (Voigt) and lower (Reuss) bounds, self-consistent average (nSCA, sSCA ) and differential effective medium estimate for strong (nDEM-sh, sDEM-sh) and weak host (nDEM-wh, sDEM-wh) are given. a) Viscosity ratio 100, aspect ratio 4. Concentration refers to the strong phase. b ) Inclusion concentration 50%, aspect ratio 4.


Anisotropic DEM

In the two dimensional anisotropic DEM, the medium is constructed in an iterative manner by

placing a given area fraction f of aligned individual inclusions of aspect ratio a b into the

host and reevaluating the host properties after each iteration step. Both, inclusion and host phase

are isotropic and the inclusion host viscosity ratio is incl hostR . The effective normal effn

and shear effs viscosities are obtained by integrating two coupled ordinary differential

equations

11

11

effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host

n s n s , eff eff effn s , and / 2a b b a . The initial values of n

and s are 1.

Anisotropic DEM






equations

11

11

effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host


and s are 1.

Anisotropic DEM






equations

11

11

effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host


and s are 1.

Anisotropic DEM






equations

11

11

effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host


and s are 1.

Anisotropic DEM






equations

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effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host


and s are 1.

Anisotropic DEM






equations

11

11

effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host


and s are 1.

Anisotropic DEM






equations

11

11

effn

n effn

effs

s effs

d Rdf f R

d Rdf f R

(1)

where , ,eff host


and s are 1.

Figure D3 Initial (a) and final configuration after a shear strain of 3(b) in a run with 30% inclusions that are 100 times weaker than the embedding matrix.

D. Microstructures

a)

0 1 2

Strain rate intensity

0.2 0.4 0.6 0.8 1.2 1.4 1.6 1.8

b)

The DEM approach does not only provide esti-mates for the effective anisotropic viscosities for a given composite configuration, but it can also be used to study the finite strain evolution of both, the effective material properties as well as the SPO. Figure D3 illustrates the evolution of a two phase composite up to a shear strain ( ) of 3 cal-culated with a MILAMIN based FEM model. The visualized field is the strain rate intensity, which shows how the deformation localizes in the weak inclusions. The inclusions become sigmoidal and the resulting structure looks similar to S-C fabrics that are often observed in natural shear zones.

The details of the inclusion shape evolution can-not be captured with the DEM approach. The un-derlying analytical solution is for elliptical inclu-sions and deviations from ellipticity are therefore ignored, which is unproblematic in dilute cases or when the inclusion phase is stronger than the host. The question arises as how well the devel-oped DEM scheme is applicable to cases such as shown in Figure 3b.

Figure D4 shows how the shear viscosity evolves in the FEM model depicted in Figure D3 as a func-tion of shear strain and compares it to the DEM prediction. The DEM scheme performs surpris-ingly well and no significant deviations between FEM and DEM are discernable up to large strains. The DEM accurately predicts an initial increase in the effective shear viscosity (up to ) and then a pronounced drop under the initial value. The increase is an effect of the development of the mechanical anisotropy due to the emerging SPO, the drop is related to the reorienta-tion of the anisotropy. This microstructural weakening may provide a viable explanation of the strain weakening that is often observed in deforming poly-phase materials. However, in the analyzed linear viscous cases the degree of weakening is not sufficient to result in a strong localization on spatial scales larger than the inclusion size and other effects such as non-linear rheology (power law), lattice preferred orientation, or dynamic recrystallization resulting in a grain size reduction should be considered in addition.


Comparison between the DEM prediction and the FEM result obtained for the Error! Reference source not found.b configuration. Error! Reference source not found. shows how the shear viscosity evolves in the FEM model

depicted in Error! Reference source not found. as a function of shear strain and compares it to

the DEM prediction. The DEM scheme performs surprisingly well and no significant deviations

between FEM and DEM are discernable up to large strains. The DEM accurately predicts an

initial increase in the effective shear viscosity effxy (up to 1 ) and then a pronounced drop

under the initial value. The increase is an effect of the development of the mechanical

anisotropy due to the emerging SPO, the drop is related to the reorientation of the anisotropy.

This microstructural weakening may provide a viable explanation of the strain weakening that is

often observed in deforming poly-phase materials. However, in the analyzed linear viscous

cases the degree of weakening is not sufficient to result in a strong localization on spatial scales

larger than the inclusion size and other effects such as non-linear rheology (power law), lattice

preferred orientation, or dynamic recrystallization resulting in a grain size reduction should be

considered in addition.

D. Microstructures

0 0.5 1 1.5 2 2.5 3

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tive

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Figure D4 Comparison between the DEM prediction and the FEM result obtained for the Figure 3b configuration.

ConclusionsThe developed anisotropic DEM model provides a better es-timate over SCA for higher concentrations of inclusions. The discrepancies between the scheme predictions reflect a fun-damental difference between the two methods: the DEM is designed for inclusion-host systems, whereas the SCA is more suitable for a poly-grain medium, where none of the phases can be considered as inclusions. Our DEM based model of the shape and mechanical anisotropy evolution provides a vi-able explanation of a strain weakening observed in poly-phase materials. The model is applicable to any deformation path and constrains constitutive laws incorporating structural evo-lution factors that are employed in large scale, geodynamic simulations.

ReferencesAustrheim, H., Putnis, C.V., Engvik, A.K., Putnis,

A., 2008. Zircon coronas around Fe-Ti oxides: a physi-cal reference frame for metamorphic and metasomatic reactions. Contributions to Mineralogy and Petrology, 156, 517-527.

Brady, J.F., Bossis, G., 1988. Stokesian Dynamics. Annual Review of Fluid Mechanics, 20, 111-157.

Dabrowski, M. 2008. Anisotropy and heterogenity in finite deformation : resolving versus upscaling. Unpub-lished Thesis, University of Oslo, Oslo, 156 pp.

Dabrowski, M., Krotkiewski, M., Schmid, D.W. 2008. MILAMIN: MATLAB-based finite element method solver for large problems. Geochemistry Geophysics Geosystems, 9, Q04030.

Fletcher, R.C. 2004. Anisotropic viscosity of a dispersion of aligned elliptical cylindrical clasts in viscous matrix. Journal of Structural Geology, 26, 1977-1987.

Jäger, P., Schmalholz, S.M., Schmid, D.W., Kuhl, E., 2008. Brittle fracture during folding of rocks: A finite element study. Philosophical Magazine, 88, 3245 - 3263.

Krotkiewski, M., Dabrowski, M., Podladchikov, Y.Y. 2008. Fractional Steps methods for transient problems on commodity computer architectures. Physics of the Earth and Planetary Interiors, 171, 122-136.

Marques, F.O., Podladchikov, Y.Y. 2009. A thin elastic core can control large-scale patterns of lithosphere shortening. Earth and Planetary Science Letters, 277, 80-85.

Milke, R. et al. 2009. Matrix rheology effects on reaction rim growth I: evidence from orthopyroxene rim growth experiments. Journal of Metamorphic Geology, 27, 71-82.

Schmalholz, S.M., Schmid, D.W., Fletcher, R.C., 2008. Evolution of pinch-and-swell structures in a power-law layer. Journal of Structural Geology, 30, 649-663.

Schmid, D.W., Abart, R., Podladchikov, Y.Y., Milke, R., 2009. Matrix rheology effects on reaction rim growth II: coupled diffusion and creep model. Journal of Meta-morphic Geology, 27, 83-91.

Schmid, D.W., Dabrowski, M., Krotkiewski, M. 2008. Evolution of large amplitude 3D fold patterns: A FEM study. Physics of the Earth and Planetary Interiors, 171, 400-408.


Mechano-chemical transformation processes

Scientific problemA characteristic example of a mechano-chemical process is stress corrosion in a windshield: A small fracture in the glass has a high stress concentration at its tip, but not high enough to cause rapid fracture motion. However, as water (hydrogen) is transported to the fracture tip, it replaces a strong covalent bond with a weaker hydrogen-bond, weakening the material, causing the fracture to propagate further. The velocity of the fracture depends on the coupling between mechanics: stress and deformation, and reaction: the replacement process, and this coupling tends to give microscopic processes a macro-scopic relevance as the rate limiting factor for reaction prog-ress.

The transformation of rock is similarly often driven by fluid infiltration, and the dynamics of such a process is to a large extent controlled by a ‘reaction front’ where the phase content and composition of the rock is changing. The reaction front is a moving interface that may be associated with both mechani-cal and chemical processes. While investigation of reactive transport in porous media has grown into a major industry, this work has so far focused mainly on the hydrodynamic and chemical aspects of front advancement, and not on the cou-pling between fluid flow, reactions, and mechanical processes such as fracture and deformation. This is clearly inadequate for the alteration of rocks with low porosities and permeabili-ties, or reactions associated with major changes in porosities or solid volume.

We have therefore developed models that address the mech-ano-chemical coupling during such processes: Fluid-initiated reaction processes lead to changes in the local stresses that induce fracturing of the rock matrix. As a result, fluids gain ac-cess to the rock matrix through the newly generated fractures. This coupled process has a first-order impact on reaction rates and also on the geometries of the generated reaction fronts. We are applying this theoretical approach, combined with field and laboratory experiments, to address serpentinization, mineral replacement reactions, and, in particular, weathering, one of the most important of all processes associated with reactive transport.

Approach and resultsRecently, we developed a numerical and theoretical framework to address the front dynamics in fracturing-accelerated reac-tion front dynamics. We have applied and tested the modeling framework to study diffusion-controlled volume changing re-actions, such as devolatilization reactions, drying, or cooling, where we found that the reaction front moves with a constant speed and a constant width (Malthe-Sørenssen et al., 2006).

This modeling framework has been extended to address gen-eral diffusion-reaction processes, including volume changes and changes in material properties as results of the progress of chemcial reactions. Volume changing reactions may lead to a decrease in volume, shrinking, such as in drying and eclog-itization, or to an increase in volume for expansion processes such as many weathering reactions.

We have applied this modeling approach to address the vol-ume-increasing processes occuring during sphereoidal weath-ering. We have demonstrated how local volume-increasing reactions may produce a large-scale hierarchical fracture pat-tern, and how this hierarchical process has a first-order im-pact on weathering rates (see Figure E1). Using the modeling framework, we obtain simulations with up to five generations of hierarchical fracturing. We have also developed a simple model for the acceleration fo the reaction rate due to hier-archical fracturing, illustrated in Figure E2. The hierarchical fracture pattern results in a rapidly growing fluid-solid contact area, and a slow diffision-reaction process progressing inward from the fluid-solid contact may therefore affect a much larger volume than in the case of an unfractured rock, where the alteration process progresses only from the outer boundaries (Røyne et al., 2008).

We are currently applying the ideas and methods from these studies to a wide range of phenomena, including serpentini-zation processes and replacement reactions, where we also observe hierarchical fracturing and accelerated reactions. For example, in collaboration with C. Putnis (Jamtveit et al, 2009) we recently applied the same techniques of analysis and mod-eling to address the replacement of leucite by analcime, which is a common process in silica-poor igneous rocks, and typi-cally results in a 10% volume increase. The fracture pattern observed on micron scale using back-scattered electron im-ages closely resemble the hierarchical fracture structure seen in comparable simulations (See Figure E3.)

E. Interface processes group


Figure E1: (a) Sphereoidal weathering pattern from Argentinian sills showing several generations of domain subdivision that are clearly formed sequentially. (b) Numerical model of reactive transport, initiated as a diffusion process from the outer boundaries. As fractures appear and connect with the outer boundaries, water also diffuses in from the fracture surfaces. The simulation shows the formation of several subdomains by various mechanisms. (c) Illustration of the reacted volume for a model where fractures are formed and conduct fluids, and for a model without fracturing,showing that fracturing leads to an accelerated reaction process.


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Figure E2: Illustration of reacted volume as a function of time in a case where there is no fracturing (top picture), and in a case where a block is subdivided when the reaction reaches a particular depth, and fluid propagates in through the fractures. The presence of fractures clearly leads to an increase in the reactive surface, and also in an increase in the reacted volume compared to the model without fracturing.



Scientific outlookWe expect this theoretical and modeling framework to form a basis for understanding bulk reaction rates in many geological systems, including for example serpentinization reactions, and we are also working on developing further experimental or geological systems that allow us to test the quantitative predic-tions of the models against data from real systems. In particu-lar, we have started studying experimental model systems of both volume reducing and volume increasing reactions, which raise challenging questions all the way down to the level of in-teratomic bonding. Over the next year, we expect to be able to bind the experimental and theoretical activities close together,

Figure E3: (a) Back-scattered electron (BSE) images of leucite crystals partly replaced by analcime demonstrates clearly developed hierarchical fracturing as shown by the magnification of the inset in (b). The line segments shows several generations of fractures. (c) Simulation of the replacement reaction also demonstrate grain partitioning and the formation of several generations of hierarchical fractures.

(a)

(b)

(c)

which will both tie the modeling methods more closely to an atomic and microscopic understanding of the processes, and, in the longer timeframe, open new directios of research.

ReferencesJamtveit, B., Malthe-Sørenssen, A. Kostenko, O. 2008.

Reaction enhanced permeability during retrogressive metamorphism. Earth and Planetary Science Letters, 267, 620-627.

Jamtveit, B., Putnis, C. V., Malthe-Sørenssen, A. 2009. Reaction induced fracturing during replacement pro-cesses. Contributions to Mineral Petrology, 157, 127-133.

Røyne, A., Jamtveit, B., Mathiesen, J., Malthe-Sørens-sen, A. 2008. Controls on weathering rates by reaction induced hierarchical fracturing. Earth and Planetary Science Letters, 275, 364-369.



The thermodynamics and roughening of solid-solid interfaces

Scientific problemAt every turn in nature we are confronted with complex pat-terns. Patterns often formed in multiphase systems by an intri-cate dynamics of mass transport, e.g. diffusion and/or advec-tion, and mass exchange between individual phases. A good share of such systems evolves in the presence of mechanical stress. In the scientific community, a few examples, in particu-lar, have been discussed intensively such as the ATG instabil-ity at the surface of stressed solids in contact with their melt or solution.

In the absence of surface tension, the instability manifests it-self by allowing small perturbations of the surface to increase in amplitude by mass diffusion from surface valleys, where the stress and chemical potential is high, to surrounding peaks where the stress and chemical potential is low. In systems where the fluid phase is replaced by another solid phase, i.e. solid-solid systems, the interface constraints alter the local equilibrium conditions. We perform research on the dynam-ics of an interface between non-hydrostatically stressed solids where the interface propagates by mass transformation from one phase into the other.

In polycrystalline materials such mass transformation appears at the grain scale during “dry recrystallization”. Other impor-tant examples of interfaces that migrate under the influence of stress include the surfaces of coherent precipitates (stressed inclusions embedded in a crystal matrix) and interfaces as-sociated with isochemical transformations.

Approach and resultsWhen two solids are compressed transverse to an interface separating them, we have shown that, if a phase transforma-tion is possible, it can lead to a morphological instability, as well as the development of fingers along the propagating in-terface (see Figure E4).

We have performed a stability analysis based on the Gibbs potential for non-hydrostatically stressed solids and have es-tablished a linear relationship between the rate of entropy production at the interface and the rate of mass exchange be-tween the solid phases. The corresponding diagrams for the morphological stability of a propagating interface reveal an intricate dependence of the stability on the material density, Poisson’s ratio and Young’s modulus, see Figure E5.

Figure E4: Simulations of the temporal evolution of solid-solid interfaces for first-order phase transitions. Panel (A) shows a simulation using densities ρupper=1.0 and ρδlower=1.05 and shear modules , Gupper=1.05 and Glower=2.0. Both phases have identical Poisson’s ratio og 0.45. Panel (B) is a simulation run with densities and shear modules similar to panel (A) but with a different Poisson’s ratio, 0.25, for both phases.



We have demonstrated that the morphological stability pro-vide important information about the type of phase transfor-mation process occurring at the interface of contacting solids and readily provide information about the material param-eters.

Scientific outlookThe interplay between the microscopic and macroscopic physics is a fundamental problem in research on complex sys-tems. The common aim of our research into the dynamics of stressed multiphase systems is to provide a link between the microstructural evolution and macroscopic system rheology. Important examples that shall be investigated in upcoming projects include the localization of compaction into bands in reactive, deformable and porous materials, the effect of anisot-ropy on solid-solid phase transformations and the slow evolu-tion of faults.

Figure E5 Example of a stability diagram for two solids in contact at a thin interface. One solid has a unit shear modulus and a unit density while the other solid has a shear modulus μ2 and densityδρ2. Both materials have a Poisson’s ratio of ¼. Regions in the diagram with positive values represent unstable growth, and negative values stable growth. Note the broken symmetry for the horizontal zero curve. This symmetry breaking has an interesting dependence on the Poisson’s ratio (See References).

While most faults evolve with a characteristic stick-slip behav-ior, a certain class of faults has a characteristic aseismic creep, i.e. the fault evolves in a way that allows it to steadily overcome the cycles of arrest controlled by the roughness and asperities. The details of the mechanisms behind this non-trivial rheology are unknown and it is important to understand the underly-ing difference between these two types of fault dynamics. A possible explanation could be related to a stress-controlled dissolution-precipitation alteration of the rough fault surface.

ReferencesAngheluta, L., Jettestuen, E., Mathiesen, J. 2009. The

thermodynamics and roughening of solid-solid inter-faces. Phys. Rev. E 79, 031601.

Angheluta, L., Jettestuen, E., Mathiesen, J., Renard, F., Jamtveit, B. 2008. Stress-driven phase transformation and the roughening of solid-solid interfaces. Phys. Rev. Lett. 100, 096105.



Research on the sensitivity to residual stresses in drying patterns

Desiccation is known to produce complex networks of shrink-age-cracks in starch-water mixtures or clays. In concrete small cracks are often formed by the preparatory drying process and by the later ingress of reactive reagents. Similarly in nature, the infiltration of fluids and chemical reagents into rocks gen-erate internal stresses that form intricate patterns of pervasive cracks.

Typically the stress is generated from local volume changes. Fractures are also observed in thin films attached to a sub-strate. Experiments on films have revealed intricate patterns ranging from the hierarchical structure typically observed in mud and concrete to spiral shaped cracks. In spin-coating a fluid droplet is added at the center of a rotating substrate and is spread by centrifugal forces to cover the full substrate. Dur-ing the drying and curing of the system, chemical bonds are formed between the coating and the substrate. In this process the coating often shrinks and tensile stresses are produced that can cause fracture. In cases where the contraction is fairly uniform, i.e. no residual shear stresses, the growing cracks typ-ically form an intricate hierarchical pattern. We have shown that small variations in the volume contraction and substrate restraint can produce widely different crack patterns ranging from spirals to complex hierarchical networks as shown in Figure E6. The networks are formed when there is no pre-vailing gradient in material contraction whereas spirals are formed in the presence of a radial gradient in the contraction of a thin elastic layer.

ReferencesCohen, Y., Mathiesen, J., Procaccia,I. 2009. Drying pat-

terns: Sensitivity to residual stresses., arXiv:0901.0797.

Figure E6: FEM simulation of shrinkage-cracks in thin elastic films attached to a substrate. Upper panel, remnant residual shear causes a crack to grow into a spiral. Lower panel, uniform stress leads to the formation of a hierarchical fracture pattern with multiple cracks advancing simultaneously.


An experimental study of stylolite formation

M.sc. thesis by Ola Kaas EriksenStylolites are features of localized dissolution in sedimentary rocks. They are planes oriented normal to the compaction di-rection and have a rough and often teeth-like surface struc-ture. The vertical spacing of individual stylolite planes are often constant within one rock sample or outcrop. There is no general agreement on how these rough planes of localized compaction form. The master thesis of Ola Eriksen presents experimental results that suggest that the characteristic dif-fusion length of solute is important for both the localization process and the vertical spacing of individual stylolite planes. Granular systems are compacted by pressure solution. The results from these experiments show that the system devel-ops spontaneously a “compaction band” structure oriented normal to the compaction direction. The spacing between the bands in this band structure is 1-2 mm, which is consistent with stylolite spacing in calcitic rock of 1-20 cm, assuming that the precipitation rate determines the characteristic diffu-sion length. A modeling study that explains the mechanisms of these ductile compaction bands is underway.

Figure E7: Deformation map of compacted granular material showing ductile compaction bands. Color scale is the local volume relative to original volume.


Figure E8: Vertical autocorrelation of the final volume matrix in Figure 1.



Extrusion of plastic crystals

M.sc. thesis by Yngve YdersbondYngve Ydersbond has performed experiments on extrusion processes. This is important in both industry and geological settings. The transition from ductile to brittle deformation in-side the extrusion die is observed as an optical contrast bound-ary, also called slip-line, between the regions in the die where stick and slip boundary conditions prevail. The dynamic of this boundary is measured in situ through optically transparent Plexiglas dies. The organic crystalline materials, Succinonitrile and Camphene, we have used are good analogs for other crys-talline material, such as aluminium. Several processes that are important in the production of extruded aluminium products have been observed. Several statistical measurements have been carried out on the slip-line, these have shown that the system are persistent or antipersistent depending on the length scale it is observed. Furthermore, the bulk and surface veloc-ity of the flowing material has been analysed and the radius of the die curvature has been systematically varied to see the effect this have on the slipline behaviour.

Energy dissipation in a simulated fault system

M.sc. thesis by Munib SarwarMovement of the earths crust builds up stresses in a fault zone, and when these stresses reaches a critical point there is slip along the fault planes causing earthquake. The energy dissi-pated in an earthquake is in plate tectonic physics partitioned into three different components Wtot = Wseismic +Wexpansion +Wfric-

tion where Wtot is the total work. The only part of the energy budget of earthquakes that can be measured directly is W seismic, the energy radiated in seismic waves. Wexpansion comes from expanding fractures and generating new surface area in the fault zone and Wfriction is the energy dissipated into heat. The last two terms can be estimated for fossil fault zones. Munib Sarwar performed experiments by scratching a halite surface with an indenter while measuring the forces (to calculate Wtot) and the thermal radiation with a sensitive, cooled IR camera (to calculate Wfriction). Careful analysis of the damage of the halite crystal allowed estimating Wexpansion. Estimating the small Wseismic to <5% he found that Wfriction is smaller than previous estimates in the literature.

Figure E9: White light interferometer topography measurements of halite surface damaged by the indenter. The typical grain size in the damage zone is 3 μm.


MasterBachelor

PGP-physics

PGP-geology

PGP-simulation

Material science

Geology

Geophysics

Mathematics

Computer science

PhysicsThe educational activities at PGP include administrating and teaching the master program, running a graduate school for PhD students, and contributing to the teaching activities at the Departments of Physics and Geology.

PGP master programThe centre hosts a two-year master program The program is based on the principle that the most effective cross-disciplinary collaborations are rooted in the excellence of the collaborators in the respective fields. In order to ensure a sufficient level of specialization, and at the same time build an interdisciplinary activity, students with Bachelor degrees in Physics, Geology, or Computer modelling are offered a common program with specializations within their respective fields.

Education

4 semester Specialization courses Master thesis Master thesis



1 semesterFYS-GEO4110 – Scientific communication and research ethics

FYS-GEO4200 – Case study in physics of geological processes

FYS-GEO4300 – Methods in physics of geological processes

10 ECTS credits 10 ECTS credits 10 ECTS credits

For 2008, the master program has the following construction:

The master project provides a practical introduction to scien-tific work and to the issues relevant to the research activities within PGP. of specialized courses are:

Physics: FYS3410 – Condensed matter physics, FYS4150 - Computational Physics, FYS4410 - Computational physics II, FYS4430 – Condensed matter physics II, FYS4460 – Disor-dered systems and percolation.

Geology: GEO4230 – Basin formation and sequence stra-tigraphy, GEO4250 – Reservoir geology, GEO4260 – Reser-voir geophysics, yGEO4620 – Seismic waves and seismology, GEO4630 - Geodynamics, Analytical methods in geochemis-try, GEO4840 - Tectonics, GEO4850 – Advanced structural geology.

Applied mathematics: MEK4550 – The finite element method in solid mechanics I, INF-MAT5370 - Trianguleringer og anv-endelser, INF5600 - Iterative methods and multigrid, INF5620 - Numerical methods for partial differential equations


The PGP master program was externally evaluated in 2008. The committee recommended to extend the scientific commu-nication part of both Fys-Geo4200 and Fys-Geo4300, and to incorporate the “ethics” from Fys-Geo4110 in Fys-Geo4200. 10 credits should be kept open for selection from a list of courses, where FysGeo4110 can be included. A main problem is a shortage of master students to the PGP program. However, Fys-Geo courses are also of interest to PhD students at PGP, other students at UiO and Guest stu-dents. Most Fys-Geo courses have a satisfactory total number of students and running the master program does not take too much extra effort. Fys-Geo4010/4030 Project task I/II, were new in 2008. These courses will mainly be available to guest students coming to PGP for a one-semester research project of 10 or 30 ECTS credits.

Teaching and examinations

Three Masters in PGP graduated and 2 PGP students defend-ed their doctorates in 2008. One new Master student started autumn 2008 and by 31 December 2008, 3 Master and 20 PhD students were registered at PGP. Our candiates have continued to be attractive employees both in industry and for recruitment to academic research fellowships. (For details, see appendix).

Fys-Geo courses

Course title Responsible Given # reg. students

Average grade

Fys-Geo4110Scientific comm. Gisler Autumn 08 7 PassedFys-Geo4200/9200Case study Austrheim Autumn 08 2/1 BFys-Geo4300Methods Dysthe Autumn 08 4 BFys-Geo4510Mechanical geomod Podladchikov Spring 08 5/7 PassedFys-Geo4520Thermodyn.geomod Podladchikov Autumn 08 2/2 Passed

Other courses

Course title Responsible /involved CommentGeo4830 H. Austrheim Autumn Geo4840 T.B.Andersen Spring Gel2130 D.W.Schmid /T.B. Andersen, M. Adamuszek Autumn Geo4810 A. Beinlich Autumn Fys-Mek1110 A. Malthe-Sørensen Spring, 140 studentsFys-Mef1110 A. Malthe-Sørensen Spring Fys2150 D.K. Dysthe SpringFys4190 A. Mathiesen SpringFys4460 A. Malthe-Sørensen Spring, 5 studentsBio4210 /Ø. Hammer, 5 hours Autumn Bio4230 /Ø. Hammer, 10 hours SpringBio4240 /Ø. Hammer, 2 hours Spring

Teaching statistics from FS by 10 March 2009:


One of PGPs aims is to provide “short and effective channels from basic research to education, industry, and the public”. Several of PGP’s core activities involve the understanding of processes relevant for the petroleum industry (see Table 1). Results from this research are presented to the industry through publications, conferences, seminars, field trips, and consulting work through collaborating companies. The topic of the 22nd Kongsberg Seminar 6-9.05.09 is on the “Physics of hydrocarbon bearing systems”. PGP research with relevance to the petroleum industry will be presented at this meeting.

PGP is actively involved in several basin modeling projects. Several of the basin modeling activities are conducted in collaboration with the petroleum industry, in particular Sta-toilHydro which is involved in both the phase transition and PetroBar projects. New development of the TECTMOD2D software has been undertaken in collaboration with Geomod-eling Solutions. PGP was further awarded a Ph.D. project from VISTA on shear heating in 2008. The project will com-mence in 2009.

A major PGP activity is related to formation, migration and cli-matic impact of hydrocarbon fluids and gases. A large project on mechanisms of primary migration was funded by PETRO-MAKS in late 2008. This project will study how hydrocarbons migration out of the source rocks and the nature of focused fluid flow in vent complexes. Our work on the LUSI mud vol-cano in Java, Indonesia, continued to attract major attention in 2008. This mud volcano erupted very close to a petroleum well drilled in 2006. The eruptions lead to the displacement

of more than 10,000 people. New modeling shows that the mud volcano likely erupted along a weakness zone created by movement of a strike-slip fault.

We are further investigating formation and venting of green-house gases from metamorphic aureoles around sill intru-sions. Unique samples from metamorphic aureoles in the Tunguska Basin, Siberia, have been collected in collaboration with Norilsk Nickel. The samples were transferred to Norway in the spring 2008. New samples have further been collected and analyzed from boreholes in the Vøring Basin off Mid-Norway and the Karoo Basin in South Africa. Our new data and theoretical models show that great quantities of hydrocar-bon gases were generated just after the emplacement of the more than 1000oC hot magma. The release of these gases in hydrothermal vent complexes may have caused major envi-ronmental changes in the End-Permian (Siberian Traps), the early Jurassic (Karoo Large Igneous Province) and the early Eocene (Northeast Atlantic Volcanic Province). The results of the volcanic basin projects have been used in collaboration with Volcanic Basin Petroleum Research (VBPR) for project work on the mid-Norwegian shelf, e.g., vent complexes on the Heidrun Field, and for industry-academic research proposals (e.g., Ocean Drilling Consortium).

Prof. Bjørn Jamtveit was elected as a board member on the VISTA programme in 2008. This programme is a joint coop-eration between the Norwegian Academy of Science and Let-ters and StatoilHydro.

Project title Funding PGP PI Resources Duration

Phase transition project: Mineral phase transitions control on basin subsidence: The role of temperature, pressure, fluids and melting

PETROMAKS Y. Podladchikov 3 Post.Doc. 2 Ph.D. 2004-2008

PetroBar project: Petroleum-related regional studies of the Barents Sea region

PETROMAKS Y. Podladchikov 1 Post.Doc. 1 Ph.D. 2006-2009

Rock instability project: Forward and inverse modeling of rock instabilities in the presence of fluids

YFF Y. Podladchikov 1 Post.Doc. 1 Ph.D. 2005-2008

Pockmark project: The geobiology of Arctic hydrothermal springs

YFF Ø. Hammer 1 Ph.D. 2004-2008

Aureole project: Hydrocarbon maturation in aureoles around sill intrusions in organic-rich sedimentary basins

PETROMAKS H. Svensen 1 Post.Doc. 1 Ph.D. 2005-2009

Paleoclimate project: Processes in volcanic basins and the implications for global warming and mass extinctions

YFF H. Svensen 2 Post.Doc. 2 Ph.D. 2007-2011

Shear heating project: The thermal evolution in sedimentary basins above large shear zones and detachments

VISTA T. B. Andersen 1 Ph.D. 2009-2011

Primary migration project: Mechanisms of primary migration PETROMAKS P. Meakin 1 Post.Doc. 2 Ph.D. 2009-2012

The African Plate StatoilHydro T. Torsvik 1 Researcher 2008-2010

Table 1. Industry-related externally funded projects at PGP in 2008.


Petromax & industry funded projects

Public relations

PGP is becoming established as a leading institution in promot-ing science to the general public. We have an active relation-ship to both national and international media with outreach both via journalists and popular science contributions from our researchers. The 2008 media statistics show that PGP re-searchers have participated in 3 national and 2 international radio programs, and have contributed to more than 30 feature articles and news stories. The highlights of 2008 include:

• ContinuedcoverageofPGPresultsontheLUSImudvolcano, headed by Adriano Mazzini. Interviews with Mazzini have been published in media like Geotimes, New Scientist, National Geographic, Süddeutsche Zei-tung, Time, and Science.

• PGP’sownpopularsciencewritingcontinues,andarti-cles by Øyvind Hammer, Sverre Planke, Bjørn Jamtveit, and Galen Gisler have been published in magazines like GEO and Meta.

• TheAndeanGeotrailProject,wherePGPresearcherOlivier Galland cycles along the Andes Mountains, started in late fall 2008 and continues in 2009. Updates are available on the web.

(From Science, 13 June 2008)


PGP is headed by a director, Bjørn Jamtveit, who is appointed in a full time position for PGP`s second 5-year period. The director, assisted by an administrative manager Trine-Lise Knudsen, has responsibility for project management, admin-istration and technical and financial delivery. The director re-ports to the board.

The scientific organization is divided in five research groups, each led by a group coordinator which reports directly to the director. All Postdocs, PhD students and Master students are associated with a research group, while senior scientists may participate in more than one group. In additon, PGP has co-ordinators for media contact, industry contact, field activities and education. The coordinators, the administrative manager and the director have regular meetings.

Organization

Coordinator

PostdocsPh.D-

studentsMS-students

C

Locali-zation

Processes

A

Geo-dynamics

Coordinator

PostdocsPh.D-

studentsMS-students

B

Fluid Processes

PGP directorJamtveit

PGP boardÅm (head)Aharony PutnisBlundy GabrielsenBouchaud Myhre

Administration -Admin. manager: Knudsen-Admin. secretary: Brastad-Lab support: Gundersen-IT support: Christopher

NRC

E

Interface Processes

D

Micro-structures

NGUAker Expl.

PGP core projects:

YFFPetrobar

IPY

Research coord.:-Industry: Planke-Education: Andersen-Media: Svensen-Field: John

Financial and administrative organizationat PGP (by December 2008)

Industry & Other

research institutions

“Start Packages”

PhD positions

Permanent positions

UiO

Coordinator

PostdocsPh.D-

studentsMS-students

Coordinator

PostdocsPh.D-

studentsMS-students

Coordinator

PostdocsPh.D-

studentsMS-students

EUMIT

International funding


Title Number Man-l. years Comment

Professors, seniors and researchers

25 17.3 1 came, 1 left

Professor emeriti 3 One added in 2008

Postdoc researchers

7 5.1 2 came, 3 left

PhD students 17w 13.5 Some not fully funded in 2008. 5 came, 2 left after PhD defence.

Techn/admin. staff at PGP

5 3.9 Including 1 tech. at Dept. of Geosci.

TOTAL: 57 39.8Guest students 4 Each staying for

at least 4 months

PGP Scientific organization 2008 PGP DirectorBjørn Jamtveit

AGeodynamics

Coordinator:S. Medvedev

Postdocs:T. John N. Simon

PhD students:M. Beuchert (YPP)S. Tanzerev (YPP)

to OctoberC. Galerne (ERN,

to October)J. Semprich (NS/JIF)

H. Vrijmoed (HA)

Master students:Magnus Løberg (YPP)

DMicro structures

Coordinator:D. Schmid

Postdocs:E. Jettestuen (BJ)

M. Dabrowski (DS, from July)

PhD students:M. Krotkiewski (DS)

Master students:Y.W. Ydersbond (DD)

EInterface

Coordinator:A. Malthe-Sørenssen

Postdocs:Christophe Raufaste

(AMS)

PhD students:S. DeVilliers (JF)A.Røyne (DKD)

L. Angheluta (JM)A. Nermoen (DD)

Master students:O.K. Eriksen (DKD)

B. Oust (JM)

CLocalization

Coordinator:K. Mair

Postdocs:S. Santucci (KM)

PhD students:V. Yarushina (YPP)

T. Bjørk (KM)

Master students:S. Munib (KM)

BFluid Processes

Coordinator:G. Gisler

Postdocs:A. Mazzinii (HS)S. Polteu (HS)

O. Galland (HS)

PhD students:F. Nicolaisen (AMS)

I. Aarnes (HS)K. Webb (ØH)

Kirsten Fristad (HS)

Master students:

Staff

As for December 31 2008, 45 employees from 14 coun-tries had their working place at PGP. The total work force constituted 39.1 man-labour years in 2008. The scientific staff has background in physics, earth science and computatonal science. Their work integrates field studies, laboratory experiments, computer simulations and theoretical calculations. PGP had x guest students staying for more than one month, performing research projects or partcipating in other PGP courses. In addi-tion, PGP has a techical-administrative staff of 3.9 man-labour years and receive ca. 2.5 man-labour years of technical-administrative support from the Department of Physics and the MN-faculty. The status of the work force is summarized below, while a complete list of staff is found in Appendix 1.

In addition to this, numerous short term visitors stayed at PGP, of whom 15 gave invited talks at the PGP ex-ternal seminar serie (see appendix).

PGP work force in 2008:


The board

PGP has a new board for its second five-year period. Its man-date is to ensure that the inventions and plans underlying the contracts between the parties are fulfilled and completed with-in the adopted time frame. The board evaluates and advises on the centre’s scientific performance and assesses recent prog-ress and future strategies. The board shall further ensure that the interaction between PGP and the host institution func-tions smoothly. The board reports to the MN-faculty.

The board consists of seven members. The chairman is a high-level manager in a major petroleum company, while four board members are scientists, two from physics and two from geosci-ences. Two board members are representatives from UiO. The board’s comprehensive management experience has played an important role in cases of strategic importance, and it also works as an advisory board in scientifc questions. This com-bined function has worked well for PGP for the first five-year period, and the model is selected also for the new board. The board meetings took place on 17 January 17 and 19-20 June.

The board members:

0,0

2,0

4,0

6,0

8,0

10,0

12,0

14,0

16,0

18,0

20,0

Professors and researchers Postdoctoral fellows Doctoral students Other personnel

Man

-labo

ur y

ears

PGP employees 2003-2008

2003

2004

2005

2006

2007

2008

Name Institution Research area Country

Knut Åm (chairman) Industry representative Norway

Prof. Amnon Aharony Tel Aviv University Physics Israel

Prof. Elisabeth Bouchaud CEA-Saclay Physics France

Prof. Jon Blundy Univ. of Bristol Geology Great Britain

Prof. Andrew Putnis University of Münster Geology Germany

Prof. Roy H. Gabrielsen Dept. Geosciences,Univ. of Oslo Geology Norway

Prof. Annik M. Myhre MN-faculty, Univ. of Oslo Dean of studies Norway


Computer and network supportPGP has invested in a simple 5 TByte server solution for back-ing up data stored on local computers. Because the amount of data produced and obtained increases faster than the avail-able network storage, many people use their local pc-disk for storing data. This is done either without any backup, or by backing up to USB disks or CD and DVD disks, but these strategies are vulnerable to failure. The server storage en-ables users to backup their data and have them available in the laboratories, in their offices or from anywhere with a se-cure network connection. The server does not have its own backup solution, but it uses redundancy and can therefore lose up to two out of its six hard drives without losing any data.

Laboratory and instrumentsThe number of experimentalists in the laboratories has been very good in 2008. Some new instruments were acquired, and the quality and selection of high level instruments have improved and are now producing good scientific results. In the interface laboratory we have invested in a new small Atomic Force Microscope (AFM) scanner system (Cali-ber from Veeco) to extend our surface imaging capability. With our scanning equipment we are now able to scan most scales and surfaces.

Infrastructure and laboratories

Equipment XY-range Z-range XY-resolution Z-resolution

AFM >90 micro m >12micro m <2 nano m 0.1 nanao m

White light interferometer 50 mm 1 mm 1 micro m 0.1 nanao m

3D needle scanner 30 x 20 cm 6 cm 50micro m - 5 mm 25micro m

3D photo scanner*) 2 m 50 cm 1/5000 FS 0.5 mm

*) Approximate values, FS = Full Scale of XY-range

The AFM system is being extended to a current mode AFM in order to map conductivity of rock samples. In order to obtain better control of the surface preparation for different experi-ments at interfaces we have also purchased a LAminar Flow (LAF) workbench that ensures a dust free environment for sample preparation.

PGP also invested in a new grayscale hi resolution and hi dynamic range camera this year. A FLI ProLine PL1600M with Class 1CCD gives us 16Mpixels and a dynamic range of 65dB and 16-bit operation. This camera enables us to capture and detect very small details and variations in various experi-ments.

Figure 1. AFM screatched this PGP logo into a CD, later it was scanned with the same AFM. The second picture shows the AFM and the process.


Figure 2. Scanning with the interferometer, the art is shown in the background.

Experimental facilitiesPGP have a total of seven laboratories (total 275m2) located from the sub-basement to the top floor. The two laboratories in the sub basement are used for experiments that require special physical conditions: The interface lab in the sub basement has good temperature and mechanical stability, a low noise venti-lation system, a high purity compressed air and water supply, a fume hood, UPS-protected electrical and vibration-free tables adjacent to the instrumentation platforms. To verify that the experiments are run in a controlled environment, we are now keeping a log of temperature and humidity.

There are no windows in the sub-basement, and employees who spend their entire day, several days a week, can feel the isolation much stronger when the environment is sterile and cold. To improve the working conditions, we have purchased art to put on the wall in the interface laboratory.

The four laboratories on the ground floor are of more gen-eral use. We have dedicated the biggest laboratory to granular experiments (“dirty and wet operations”) to keep the other laboratories from getting filled with dust. The temperatures in these rooms are very unstable, especially in the summer there can be huge fluctuations during the day. This is the reason why the long term experiments or those dependent on stable temperatures are only run in the sub-basement and not in any of these laboratories.

One laboratory on the ground floor is more or less dedicated to the infrared camera. This has been used in friction/scratch-ing and thermal conductivity experiments and has been used frequently during the entire year. The only laboratory on the 4th floor is mainly being used by I. Giæver for his experiments. Since this laboratory is located close to the offices, it is also convenient for smaller matters like microscopy.


PGP had a total income of 42 479 thousand Norwegian kro-ner (kkr) in 2008, and total expences of 35 258 kkr. 7 221 kkr were transferred from 2007 for future salary obligations and delayed research activities. UiO grants and permanent pos-tions constituted 30 % of the income to PGP, the SFF grant was 41 % of the income, and the remaining income came from other NRC projects (26 %) and international funding and oth-

Finances

Accounting 2008Type of financing UiO NRC NRC Inter-

national funding

Other private grants

GRAND TOTAL

Accoring to the long-term contract with NRCProject number

Basis PGP

SFF Other projects

EU, MIT ChevTex, StatoilHydro, Aker Expl

Income

UiO/MN grant 4 974 4 974 9 274UiO permanent positions 5 323 5 323SFF from NRC 14 036 14 036 14 036International funding (EU, MIT) 92 92 600Other NRC grants 1 503 7 590 9 093 7 283Other/private grants 1 000 1 000 2 531SUM income 11 800 14 036 7 590 92 1 000 34 518 33 724Transfer 2007-2008 2 931 1 735 2 671 624 7 961 Transfer between accounts -2 000 2 000 0 SUM income incl. transfer 12 731 17 771 10 261 92 1 624 42 479

Costs

Temporary positions 4 136 10 575 3 334 934 18 979 Overhead (-inn/+out) 135 1 221 861 143 2 360 SUM temp. pos+overhead 4 271 11 796 4 195 1 077 21 339 23 639UiO permanent positions 5 323 5 323Investments 35 503 100 638 1 820Operating costs 427 3 157 3 869 92 413 7 958 8 265SUM operating costs & inv. 462 3 660 3 969 92 413 8 596 10 085SUM Total expences 10 056 15 456 8 164 92 1 490 35 258 33 724

Transfer 2008-2009 2 787 2 203 2 097 0 134 7 221 Balance -112 112 0 0 0 0 0All numbers are in 1000 NOK (kkr)

Comments: Transferred money represent future salary obligations and late activities. UiO-Basis includes the Petrobar project granted to Dept. of Geology. The total funding in long term contract with NRC also includes 9723 kkr in overhead expences covered by UiO.

er private grants (3 %). Total income pr. man-labour year was 1.067 kkr, while the total expences pr. man-labour year was 886 kkr. Operating costs pluss investments pr. man-labour year were 216 kkr. Temporary and permanent posions consti-tuted 61 % and 15 % of the costs, respectively, and operating costs and investments constituted the remaining 24 %.


PGP is on track financially also in 2008. The center had 794 kkr higher income than anticipated in the long term fund-ing plan of the contract with the Norwegian Research Coun-cil. The financiation from other NRC projects was substan-tially higher than anticipated, but the financiation from other private grants was lower. EU funding for 2007 will enter the budget in 2008 and EU funding is low, but increasing at PGP. The investments and operating costs were lower than antici-pated and this is connectet to a long-term sick leave of one of the senior staff members.

PGP personell are involved in 5 new projects in 2008.Håkon Austrheim is working on CO2 sequestation and is the UiO project leader in an EU-financed project coordinated by A.

Putnis in Münster, Germany. Torgeir B. Andersen is a co-su-pervicor for a PhD student at University of Oslo, payed by a YFF grant to Susanne Buiter at NGU (The Norwegian Geo-logical Survey). Henrik Svensen has a grant from MIT, USA, covering analytical expences on rock samples from Siberia. A grant from Statoil-Hydro to NGU and Trond H. Torsvik, coveres most salary expences for a senior researcher at PGP for the period 2008 to 2011. Dag K. Dysthe has a UiO “Start package” for the period 2008 to 2010. PGP also received two new PhD postions from the MN-faculty, one in co-operation with the Department of Geology, and one with the SFF-center Centre of Mathematics for Applications, CMA. The complete project portifolio for 2008 is given in the appendix.

New projects from 2008

Interntat. fundingfrom EU

Coordinator:A. Putnis,Münster

EU:DELTA-MIN

H. Austrheim(2008-2011)ca. 3 700 kkr

2 PhDstudentsfrom 2009

NRCYFF to Buiter,

NGU

T.B.Andersen (2008-2011)

PhD student:K. Ghazian

Start packageTiltak 150102

D.K. Dysthe2008-2011

TOT: 863 kkr(incl. 25% Granted

from PGP)

UiOfinanciation

NGU

T. Torsvik(2008-2010)

2100 kkr

Researcher:S. Medvedev

Otherprivate grants

2 new PhD positions(2008-2011)D. Schmid:

M. Krotkiewski(PGP-CMA)Austrheim:A. Beinlich(PGP-DG)

TOT: 3846kkr

MIT:Siberian

Traps

H. Svensen(2008-2011)

TOT :US$ 93330

Internat. funding


Appendices 2008 List of staff .............................................................642008 Student list .............................................................662008 Numerical models ............................................... 682008 Fieldwork .............................................................. 692008 Project portfolio .................................................. 702008 Invited talks ......................................................... 722008 Experimental laboratory activities................... 722008 Production list ..................................................... 74

Appendices


List of staff

Name Title % pos. Project From To Man-labour year

Background

Permanent postions, financed directly from UiO

Aharony Amnon Professor 20 NA 01.02.2003 NA 0,2 Israel

Austrheim Håkon Professor 75 NA NA NA 0,8 Norway

Andersen Torgeir B. Professor 75 NA NA NA 0,8 Norway

Corell, Gro Adm. 25 NA NA NA 0,3 Norway

Feder Jens Professor 75 NA NA 31.01.2009 0,8 Norway

Jøssang Torstein Professor emer. 75 NA NA NA 0,8 Norway

Neumann Else-Ragnhild Professor emer. 75 NA NA NA 0,8 Norway

Malthe-Sørenssen Anders Professor 75 NA NA NA 0,8 Norway

NN Tech. Assist. from Dept. P. Techn. 200 NA NA NA 2,0 Norway

Røyne Anja PhD student 100 NA 08.08.2005 1,0 Norway

Schmid Daniel W. Senior 75 NA 01.04.2003 31.01.2013 0,8 Switzerland

Financed from Basis PGP

Angheluta Luiza PhD student 100 0 16.10.2006 15.10.2009 1,0 Romania

Beinlich, Andreas PhD student 100 01.09.2008 31.08.2012 0,3 Germany

Dysthe Dag Professor 100 NA 01.01.2006 NA 1,0 Norway

Podladtchikov Yuri Professor 100 0 01.07.2003 NA 1,0 Russia

Krotkiewski Marcin PhD student 100 142042 01.01.2008 31.12.2011 1,0 Poland

Nermoen Anders PhD student 100 0 21.08.2006 20.08.2010 1,0 Norway

Semprich Julia PhD student 100 0 01.05.2007 30.04.2010 1,0 Germany

Simon Nina S.C. Postdoc 100 121124 01.04.2007 31.01.2010 1,0 Germany

Financed from SFF

Adamuzek Martha PhD student 100 142042 22.08.2008 21.08.2011 0,4 Poland

Beuchert Marcus PhD student 100 142042 10.10.2008 31.12.2008 0,2 Germany

Bjørk Torbjørn stipendiat 100 142042 01.01.2008 1,2,08 0,1 Norway

Bjørk Torbjørn PhD student 100 142042 01.02.2008 31.01.2011 0,9 Norway

Brastad Karin konsulent 100 142042 01.09.2003 31.01.2010 1,0 Norway

Cristopher Jesmine Techn. 60 142042 03.05.2006 31.12.2012 0,6 Norway

Dabrowski Marcin PhD student 100 142042 01.04.2008 30.06.2008 0,3 Poland

Dabrowski Marcin Postdoc 100 142042 01.07.2008 31.06.2010 0,5 Poland

De Villiers Simon PhD student 100 142042 01.03.2008 0,3 South Africa

Fletcher Ray Professor 20 142042 01.01.2006 31.12.2008 0,2 USA

Galerne Christophe PhD student 100 142042 01.01.2008 30.03.2008 0,3 France

Galland Olivier Postdoc 100 142042 01.07.2008 31.11.2008 0,5 France

Gisler Galen Senior 100 142042 01.04.2006 31.01.2013 1,0 USA

Gundersen Olav Techn. 100 142042 08.09.2003 31.12.2013 1,0 Norway

Hammer Øyvind Senior 50 142042 01.02.2003 31.01.2013 0,5 Norway

Hartz Ebbe Hvidegård Professor 20 142042 01.02.2007 31.01.2010 0,2Norway/Denmark

Jettestuen Espen Postdoc 100 142042 01.01.2008 31.12.2008 1,0 Norway

Jamtveit Bjørn Professor 100 142042 01.02.2003 31.01.2010 1,0 Norway

John Timm Postdoc 142042 Lønnet av Aker Exploration 0,0 Germany

John Timm Postdoc 100 142042 01.11.2008 31.12.2008 0,2 Germany

Knudsen, Trine-Lise Adm. 100 142042 17.06.2007 1,0 Norway


Mair Karen Senior 100 142042 01.01.2005 31.12.2012 0,4 Great Britain

Mathiesen Joakim Ass. Professor 100 142042 01.02.2009 NA 1,0 Denmark

Meakin, Paul Professor II 29 142042 01.01.2008 31.12.2008 0,3 USA

Planke Sverre Senior 20 142042 01.02.2003 31.01.2013 0,2 Norway

Raufaste, Christophe Postdoc 100 142042 01.01.2008 31.12.2009 1,0 France

Renard Francois Professor 20 142042 01.04.2003 31.03.2011 0,2 France

Santucci, Stephane Senior 100 142042 01.01.2008 31.12.2008 1,0 France

Souche, Alban vit.ass 100 142042 01.10.2008 31.12.2008 0,3 France

Svensen Henrik Senior 100 142042 01.09.2005 31.12.2012 1,0 Norway

Tanzerev Evgenyi PhD student 100 142042 11.12.2007 31.01.2008 0,1 Russia

Torsvik, Trond Helge Professor 20 142042 01.04.2007 31.03.2010 0,2 Norway

Vrijmoed Hans PhD student 100 142042 26.09.2008 31.12.2008 0,3The Netherlands

Yarushina Victoria PhD student 100 142042 18.10.2008 31.12.2008 0,2 Russia

Financed from other NRC projects

Nicolaisen Filip Ferris PhD student 100 142404 01.09.2008 31.11.08 0,3 Norway

Beuchert Marcus PhD student 100 142405 10.10.2005 09.10.2008 0,9 Germany

Dabrowski Marcin PhD student 100 142405 01.04.2005 31.03.2008 0,3 Poland

Yarushina Victoria PhD student 100 121114 18.10.2005 17.10.2009 0,8 Russia

Webb Karen Elizabeth PhD student 100 121116 20.06.2005 30.09.2008 0,8 Great Britain

Aarnes Ingrid PhD student 100 142561 01.10.2006 30.09.2009 1,0 Norway

Polteau Stephane Postdoc 100 142561 01.09.2006 31.01.2008 0,1 France

Polteau Stephane Forsker 50 142561 01.02.2008 31.03.2009 0,5 France


Galland, Olivier Postdoc 100 142953 01.01.2008 31.06.2008 0,5 France

Mazzini, Adriano Forsker 100 142953 01.10.2007 30.09.2009 1,0 France

Polozov, Alexander Førsteaman. 2 20 142953 01.09.2007 31.01.2009 0,2 Russia

Fristad, Kirsten PhD student 100 142953 11.06.2008 10.06.2011 0,5 USA


Financed from private grants

Medvedev Sergei Senior 100 01.01.2008 31.12.2008 1,0 Russia

Souche, Alban vit.ass 100 420853 01.08.2008 31.9.2008 0,2 France

Visiting guest students

Fristad, Kirsten Guest student 100 01.01.2008 30.05.2008 0,4 USA

Latini, Andrea Guest student 100 01.08.2008 20.12.2008 0,4 Italy

Malvoisin, Benjamin Guest student 100 01.02.2008 18.07.2008 0,4 France

Souche, Alban Guest student 100 10.01.2008 20.06.2008 0,4 France

Professors 8,8

Senior researchers 8,5

Postdocs 5,1

PhD students 12,8

Other 5,9


Appendices

PhD students

Name Main supervisor Topic Financiation

1 Aarnes, Ingrid Svensen Metamorphism around sill intrusion NRC

2 Adamuszek, Marta Schmid Fold and thrust belts CoE, NRC

3 Angheluta, Luiza Mathiesen Pattern formation, stylolites NRC

4 Beinlich, Andreas Austrheim CO2-sequestration UiO; with Dept. of Geosci.

5 Bjørk, Torbjørn Mair Faults and fault rocks CoE, NRC

6 Beuchert, Marcus Podladchikov Crust-mantle interaction NRC

7 De Villiers, Simon Feder Crumpled sheets NRC

8 Dabrowski, Marcin* June 08 Anisotropy and geterogeneity in finite deformation - resolving vs. Upscaling

NRC

9 Fristad, Kirsten Svensen NRC

10 Galerne, Christopher Neumann Sill intrusion NRC

11 Krotkiewski, Marcin Schmid Computational geodynamics UiO, with CMA

12 Nermoen, Anders Podladchikov Particle flow in microphores UiO, MN-fac

13 Nicolaysen, Fillip Malthe-Sørensen

Numerical simulations of hydrothermal vent NRC

14 Røyne, Anja Weathering UiO; MN-fac

15 Semprich, Julia Podladchikov Basin formation NRC (Petromaks at Dept. of Geosci)

16 Souche, Alban Andersen The thermal evolution in sedimentary basins Vista

17 Tanserev, Evgeniy** Podladchikov Time-reverse methods in modelling of diffusive, convective and reactive transport

NRC

18 Vrijmoed, Johannes Podladchikov Fracturing, metamorphism and metasmonatism at ultra-high pressure

UiO, MN-fac

19 Webb, Karen Hammer Marine biogeology NRC

20 Yarushina, Victorya Podladchikov Computational geophysics NRC

* dissertation 19 June 2008, ** dissertation 18 September 2009

Master students

Name Main superv. Topic Background

1 Løberg, Magnus B. Podladchikov Wave phenomena in chemically reactive porous media Mathematics

2 Nyhagen, Daniel S. From January 2009 Mechanics

3 Oust, Bodil Mathiesen Diapir modelling Physics

4 Paulsen, Kristin Schmid Physics

Student list


Previous PhD students

Name Examination Position after PGP

1 Jettestuen, Espen June 04 Postdoc, PGP

2 Harstad, Andreas January 06 DNO

3 Bræck, Simen September 07 Høgskolen i Oslo

4 Iyer, Karthik December 07 Postdoc, Univ. Kiel

5 Rohzko, Alexander December 07 EMGS ASA, Trondheim

6 Uri, Nina March 2006 EMGS ASA

Previous Master students

Name Exam. date Employment after PGP

1 Munib Sarwar Oct 08 PGP short term

2 Ola K. Eriksen Oct 08 VBPR

3 Yngve W. Ydersbond Oct 09 Vindteknikk as

4 Tomas Husdal May 07 Bodin Vidregående skole

5 Siri A.L. Sali December 04 Geoservices SA

6 Camilla Haave February 05 Geoservices SA

7 Torkil Sørlie Røhr June 05 PhD, Dept. of Geology

8 Martin Søreng August 06 Telenor

9 Berit Mattson February 05 Petroleum Geoservices SA

10 Anders Nermoen June 06 PhD, PGP

11 Solveig Røyjom June 06 StatoilHydro

12 Grunde Waag June 06 EMGS

13 Ingrid Aarnes June 06 PhD, PGP

14 Eoin McGrath February 05 Univ. College Dublin

15 Torbjørn Bjørk December 06 PhD, PGP

16 Helena K. Nygård December 06 Studies, UiO

17 Kirstein Haaberg December 06 EMGS

18 Hilde Henriksen May 07


Appendices

Particular characteristics of geological processes such as com-plex and strongly varying material properties in space and time, development of strong localization, large strain, multi-physics and multi-scale requirements render commercial soft-ware packages not applicable or make their application as much or more tedious than the development from scratch.

Numerical models

Name Developers Purpose / Method

CBI Schmid et al. 2D and 3D implementation of the Cahn/Hilliard equation to study mineral exsolution.

BILAMIN Krotkiewski et al. 3D deformation model for large strain. Body fitted meshes, finite element method implemented for large cluster systems, can solve systems with 200’000’000 unknowns.

GranMaS Nicolaisen 2D Granular Material Simulation. Discrete element code for simulating granular motion combined with fluid diffusion in a porous media.

Kirbestr Rozhko 2D finite difference code to model propagation of fractures driven by filtration of fluid in a porous medium. Darcian filtration of fluid in a medium with a nonlinear poro-elasto-plastic constitutive relationship. Used to study venting.

LiToastPhere Hartz et al. 1D code that models the deformation in a deforming lithosphere. Includes deformation, frictional heat, lithospheric strength, geothermal gradient, tectonic overpressure, mineral phase transitions, and uplift and subsidence as a result of force, energy and mass balanced thinning or thickening.

MILAMIN* Dabrowski et al. 2D general purpose finite element code with body fitted meshes. 1 million unknowns in 1 minute.

OS_Wave & OS_Flow Krotkiewski et al. Operate split based 3D methods for wave propagation and fluid flow. Structured grids with billions of unknowns solved in minutes.

Proshell Medvedev Shell implementation of the finite element method to study the interaction between deformation and surface processes.

ReactDem Malthe-Sørenssen 2D Discrete Element Model coupled to diffusion-reaction and fluid-flow solvers

StokesDyn Jettestuen #D Stokesian dynamics model for deofrming particle suspensions

Table 1 (Incomplete) list of numerical models developed at PGP


2008 Registered field work

A short summary of field activities giving: a) Location and duration; b) Participants from PGP in bold; c) Comment

1a) “Karelian Craton Transect” (Finland, Russia) Field trip as part of IGC 2008. 28.07 – 04.08b) Marcus Buchert, Leaders: Peltonen, Holtta & Slabunov

2a) Sweden-Norway IGC33 Post-Conference Excursion 34, Tectonostratigraphic transect through the Caledonides. (including partly leadership).b) J.C.Vrijmoed

3a) FysGeo 4300, Oslo area, 04.09.2008b) T.B. Andersen, Andrea Latini, Marta Adamuszek, Kris-tin Paulsen, Filip Nicolaisen, Alaban Souche, Heidi Hefre Haugland.

4a) Field course in Fys-Geo 4200, Leka, Nord Trøndelag, Røros, Sør-Trøndelag 14.-20.09.2008,b) Håkon Austrheim, Andrea Latini, Christophe Raufaste, Andreas Beinlich, Kristin Paulsen.

5a) Field work Solund, 25.09-29.09.2008b) Håkon Austrheim, Andreas Beinlich.

6a) Field work Neuquen province, Argentina, 25.3 – 13.4.b) Henrik Svensen, Adriano Mazzini, Olivier Galland, Bjørn Jamtveit, Sverre Planke, Fernando Corfu

7a) Field work, East Greenland, July - Augustb) Ebbe H. Hartz, Niels Hovius (University lecturer at Cam-bridge University) and their sons Torjus and Miro.c) Book on childrens meeting with the Arctic

8a) Salton Sea, California, 8 - 13.12b)Adriano Mazzini, Stephan Polteau, Anders Nermoen, Kirsten Fristadc) Work on hydrothermal venting


Appendices

UiO financiation, Basis

Startpackage Anders Malthe-Sørenssen (104025)

PI: AMS

Funding, kkr: 400

Comment: Transferred kkr from 200

Startpackage Joachim Mathiesen (104024)

PI: Joachim Mathiesen

Funding, kkr: 400


Startpackage Dag K. Dysthe (150102)

PI: Dag K. Dysthe

Funding, kkr: 158


PhD positions (410000)

Funding, kkr: 1 227


Research strategy

Funding, kkr: 2 000

Research school, Podladchikov (104020)

Funding, kkr: 789

UIO FINANCIATION: 4 974

Permanent positions (salary costs only)

Funding, kkr: 5 323

TOTAL UIO FINANCIATION: 10 297

SFF grant

Funding, kkr: 14 036


Petromax Petrobar, 175973/S30

PI: J.I. Faleide DG/Yuri Podladchikov, UiO basis, tiltak 104026

Funding, kkr: 1 503


Other NRC projects

YFF grant Forvard and inverse Yuri Podladchikov, 162741/V00

PI: Yuri Podladchikov, UiO project 121114

Funding, kkr: 113

Comment: 56 kkr kkr is kept back until final report.

YFF grant Øyvind Hammer, 162990/V30

PI: Hammer, UiO project 142919

Funding, kkr: 678

Comment: Transferred 179 kkr from 2008. Terminates 30.10.09.

Mineral phase transition, 163464/S30

PI: YPP, UiO project 142405

Funding, kkr: 410

Comment:

Emplacement, 159824/V30

PI: ERN, UiO project 142249

Funding, kkr: 215

Comment: Terminates 31.12.08

YFF grant Henrik Svensen 180678/V30

PI: Henrik Svensen, UiO project 142953

Funding, kkr: 2 312

Comment: Revised financiation plan from 2008

IPY grant Torjus and Miro explore Arctic, 182146/S30

PI: Ebbe H. Hartz, UiO project 142919

Funding, kkr: 197

Comment: Money hold back for final reporting 1 May 2009.

Petromax Vents Anders Malthe-Sørenssen, 163469/S30

PI: AMS, UiO project 142404

Funding, kkr: 510


Eurora: Large igneous provinces

PI: Henrik Svensen, UiO project x

Funding, kkr: 0

Comment: Money inn in 2009, after reporting

Petromax Hydrocarbon in aureoles 169457/S30

PI: Henrik Svensen, UiO project 142561

Funding, kkr: 1 652

Comment: Sluttrapport 30.9.09, projekt til avslutning 31.3.2010

TOTAL FINANCIATION, OTHER NRC PROJECTS : 7 590

Project portfolio 2008


International funding

EU: Delta-min

PI: Andrew Putnis (Munster)/ Håkon Austrheim. UiO project 650010

Funding, kkr: 0

Comment: Money for 2008 og 2009 enters in January 2009

MIT: Siberian Traps

PI: Henrik Svensen, UiO procject 690249

Funding, kkr: 92

Comment: Transferred 92 kkr from 2008. * in $

TOT. FINANCIATION, INTERNAT. GRANTS: 92

Other private

NGU: African Plate

PI: Trond H. Torsvik. UiO project 211445

Funding, kkr: 700

Comment:

Aker Exploration

PI: be H. Hartz, UiO procject 420945

Funding, kkr: 300

Comment: Transferred 86 kkr from 2008. Terminates 31.12.09.

TOT. FINANCIATION, PRIVATE GRANTS : 1 000

Appendices


November 13: Claudia Trepmann Ruhr-Universitaet Bochum. Steady state versus non-steady state flow - the microstructureal record of experiment and nature.

October 9: Julien Scheibert (CEA-SACLAY Paris). Stress/strain field measurements at a multicontact frictional interface.

May 15: Eystein Jansen Bergen. Past and future climates.

May 22: Olivier Vidale Grenoble, France.

May 29: Jean-Pierre Gratier Grenoble, France. Pressure solu-tion creep law from indentation experiments and application to fault permeability and strength evolution during seismic cycle.

June 10: Jean-Christophe Geminard Lyon, France. Intermittant gas-flow and bursting bubbles into a non-newtonian fluid.

June 12: Osvanny Ramos Lyon, France. Avalanche prediction in Self-organized systems.

June 23: Ran Holtzman Berkeley, California. April 3: Volker Oye NORSAR. Estimation of small-scale het-erogeneities inferred from microearthquake observations at the San Andreas Fault Observatory at Depth (SAFOD).

March 27: David Smith Paris, France. Selected topics on apply-ing Raman spectroscopy and micro-mapping to jadeite/coesite/diamond/zircon questions in HPM/UHPM terrains in Greece, Guatemala, Kazakstan & Norway.

February 29: Richard Schultz Reno, Nevada USA. What con-trols displacement-length scaling of geologic structures?

February 28: Frederique Rolandone France. The evolution of the brittle ductile transition during the earthquake cycle: con-straints from the time-dependent depth distributions of after-shocks.

February 14: Steffen Abe RWTH Aachen University, Germany. DEM simulations of normal faulting in a cohesive material.

January 31: Karel Schulmann Strasbourg, France. Vertical ex-trusion and horizontal channel flow: key mechanisms of exhu-mation in large hot. orogens

January 17: Ritske Huismans, Bergen. Complex Rifted Margins Explained by Dynamical Models of Depth-Dependent Litho-spheric Extension.

Invited talks 2008 Experimental laboratory activities

The number of experimental users and of experimental activi-ties is increaseing The following gives an overview of the ac-tivities, which cover a broad range of processes and geological applications, from the micro-scale to the geological scale. In addition to this, the experimental lab engineer Olav Gunder-sen knows all the experimental equipment and facilities and is of considerable help in the development of new experimental projects and setups.

1. Stéphane SantucciFriction/fracture processesThis project is a part of the fault and fracturing project. It fo-cuses on the detailed quantification of the processes involved during faulting. It consists of the development of simultaneous optical – combining direct observations and Infrared Imaging - and acoustic tracking of friction and fracture processes.

2. Munib Sarwar (Master student, supervisor: Dag Kristian Dysthe and Karen Mair)Energy dissipation in a simulated fault systemPart of the fault and fracturing project, dealing with thermal imaging and topographic analysis of a halide crystal (NaCl) submitted to friction. Such an experimental approach provides good constraints on the energy dissipation during fault mo-tion. Thermal imaging of the frictional surface during scratch-ing gives a temperature profile around the indenter which is used to estimate the amount of energy converted into heat.

3. Anja Røyne (PhD student, supervisor: Dag Kristian Dysthe)Double torsion testing of subcritical crack growth in calcite sin-gle crystalsThe aim of this project is to understand the mechanical effect of migrating fluids through rocks, with particular applications to weathering processes and fluid-assisted metamorphic reac-tions. One experimental approach consists of looking at reac-tion fronts in a hydrating salt. Another approach focuses on subcritical cracking in calcite.

4. Christophe RaufasteVolume changes in solids induced by chemical alteration The project deals with the coupling between mechanics and chemical alteration. Different “model” materials are investi-gated to understand the effect of volume changes induced lo-cally by chemical reaction. Experiments are performed under optical microscope and the interface of reaction is imaged down to a resolution of a few microns.


Appendices

5. Olivier GallandMechanisms of shallow magma emplacementThe experimental setup allows a coupled monitoring of mag-ma pressure, deformation of model surface, and the 3D shape of resulting intrusion. Such a dataset allows a precise quanti-fication of simulated processes. The aim is to understand the physical processes governing the emplacement of magma into the upper crust.

6. Anders Nermoen (PhD student, Supervisor Yuri Podladchikov)Particle dynamics of microscopic poresIn order to study the fluid induced deformation we have per-formed four experiments during 2008: 6.1. Shearing as an effective triggering mechanism for the for-mation of piercement structures in granular media. Applied to the Lusi mud volcano in Indonesia (3D).

6.2. Chimney formation; patterns produced when a bi-modal mixture of grains segregate in the air-induced fluidized state. Quasi 2 D geometry.

6.3. Dry-ice experiments consider the case when a chemical compound emplaced in a sedimentary/granular package re-acts causing a rise in the local fluid pressure. Pipes form when heat is introduced to the system triggering the sublimation of the dry ice. This experiment serves as a natural lab-analogue to pipe formation in the sill emplacement project.

6.4. The stress state of a packing of granular materials is af-fected by the interstitial fluid flow, through the so-called seep-age forces. We have performed a series of experiments where we study the de-stabilization of a sand pile triggered by the imposed fluid flow. 6.5. Experiments on crystallization pressure induced fractur-ing of 2D synthetic ‘rocks’, made by a mixture of water and vanish and glass beads. Salt crystals grow within the beads. We are hoping to btain a direct observation of deformation

7. Delphine Croizé (PhD student at Geosciences, supervi-sors: Dag Kristian Dysthe, François Renard, Knut Bjørlyk-ke, Jens Jahren)Calcite pressure solution: single-contact experimentsProcesses controlling compaction, i.e., porosity reduction, in carbonate sediments are still poorly understood, and chemical compaction, involving pressure solution, need to be studied. Two sets of experiments are realized in which deformation of carbonate is measured as a function of time, stress, grain size or fluid in presence. This is done at the grain scale. The obser-vation of the contact is done through reflected light, this make

possible to look at the contact and the Newton rings gener-ated by it. Following the Newton rings displacement enables the determination of the rate of calcite dissolution as a func-tion of the applied stress.

8. Matthieu AngeliSalt hydration with temperature Imbibition of porous media Salt crystallization during drying of porous mediaSalt crystallization is a very damaging process for the porous sedimentary stones. This process is partly responsible for ero-sion or for the degradation of cultural heritage. It is highly dependent on the type of rock and the type of salt. The main goal is to study how these crystallization processes occur in the porous media, via the help of 2D glass models. For this we observe the crystallization and phase changes of different salts (sodium chloride; sodium sulphate, magnesium sulphate...), and how this crystallization affects the mechanical strength of the media and its fluid flow properties.

9. Ola Kaas Eriksen (Master student, supervisor: Dag Kris-tian Dysthe)An experimental study on the growth of stylolitesThe aim of this project was to simulate experimentally the growing of stylolites. The main part of this work was compact-ing experiments with model materials where pressure solution is the important process. The results from these experiments show that the system develops spontaneously a “compaction band” structure oriented normal to the compaction direction. Granular systems are compacted by pressure solution.

10. Yngve W. Ydersbond (Master student, supervisors: Dag Krystian Dysthe and Jens Feder)Crack front dynamicsExperiments on extrusion processes. The transition from duc-tile to brittle deformation inside the extrusion die is observed as an optical contrast boundary, also called slip-line, between the regions in the die where stick and slip boundary condi-tions prevail. The dynamic of this boundary is measured in situ through optically transparent Plexiglas dies. We have used the organic crystalline materials, Succinonitrile and Camphene. Furthermore, the bulk and surface velocity of the flowing ma-terial has been analysed and the radius of the die curvature has been systematically varied to see the effect this have on the slipline behaviour.

11. Dysthe with Nermoen, Yderbond, Kaas and Munib The ‘PGP science museum’, a series of demonstration experi-ments.


Publications in international journals 2008Aarnes, I., Podladchikov, Y.Y., Neumann, E.-R.1. 2008. Post-em-placement melt flow induced by thermal stresses: implications for differentiation in sills. Earth and Planetary Science Letters, 276, 152-166.

Alvey, A., Gaina, C., Kusznir, N.J., 2. Torsvik, T.H. 2008. Integrated Crustal Thickness Mapping & Plate Reconstructions for the High Arctic. Earth and Planetary Sciences, 274, 310-321.

Andersen, T.B., Mair, K., Austrheim, H.O., Podladchikov, Y.Y., 3. Vrijmoed, J.C. 2008. Stress-release in exhumed intermediate-deep earthquakes determined from ultramafic pseudotachylyte. Geol-ogy, 36, 995-998.

Angheluta, L., Jettestuen, E., Mathiesen, J., Renard, F., Jamtveit, 4. B. 2008. Stress-driven phase transformation and the roughening of solid-solid interfaces. Phys. Rev. Lett., 100, 096105.

Austrheim, H.,5. Prestvik, T. 2008. Rodingitization and hydration of the oceanic lithosphere as developed in the Leka ophiolite, north central Norway. Lithos, 104, 177-198.

Austrheim, H.,6. Putnis, C.V., Engvik, A.K., Putnis, A. 2008. Zircon coronas around Fe-Ti oxides: a physical reference frame for meta-morphic and metasomatic reactions. Contributions to Mineralogy and Petrology, 156, 517-527.

Burke, K., Steinberger, B.,7. Torsvik, T.H., Smethurst, M.A., 2008. Plume Generation Zones at the margins of Large Low Shear Velo-city Provinces on the Core-Mantle Boundary. Earth and Planetary Sciences, 265, 49-60.

Dabrowski, M., Krotkiewski, M., Schmid, D.W.8. 2008. MILAMIN: MATLAB-based FEM solver for large problems. Geochemistry, Geophysics, and Geosystems, 9, Q04030.

Engvik, A.K., 9. Andersen T.B., Wachmann, M. 2008. Inhomogene-ous deformation in deeply buried continental crust, an example from the eclogite-facies province of the Western Gneiss Region, Norway. Norwegian Journal of Geology, 87, 373-389.

Engvik, A.K., Putnis, A., Fritz Gerald, J.D., 10. Austrheim, H. 2008. Albitization of granitic rocks: The mechanism of replacement of oligoclase by albite. The Canandian Mineralogist 46,1401-1415.

Ferrando, S., Frezzotti, M.L., 11. Neumann, E.-R., De Astis, Peccerillo, A., Dereje, A., Gezahegn, Y., Teklevold, A. 2008. Composition and geothermal structure of the lithosphere beneath the Ethiopian Pla-teau: evidence from mantle xenoliths in basanites, Injibara, Lake Tana Province. Mineralogy and Petrology, 93, 47-78.

Galerne, C.Y., Neumann, E.R., Planke, S12. . 2008. Emplacement Mechanisms of Sill Complexes: Information from the Geochemi-cal Architecture of the Golden Valley Sill Complex, South Africa. Journal of Volcanology and Geothermal Research, 177, 425-440.

Ganerød, M., Smethurst, M.A., Rousse, S., 13. Torsvik, T.H., Prest-vik, T. 2008. Reassembling the Paleogene-Eocene North Atlantic Igneous Province: new paleomagnetic constraints from the Isle of Mull, Scotland. Earth Planet Sci. Lett., 272, 464-475.

Galland, O.14. , Cobbold, P. R., Hallot, E., de Bremond d’Ars, J. 2008. Magma-controlled tectonics in compressional settings: insights from geological exam. Bollettino Della Società Geologica Italiana, 127, 205-208.

Gisler, G.R. 15. 2008. Tsunami Simulations. Annual Review of Fluid Mechanics, 40, 71-90.

Glodny, J., Kûhn, A., 16. Austrheim, H. 2008. Geochronology of fluid-induced eclogite and amphibolite facies metamorphic reactions in a subduction–collision system, Bergen Arcs, Norway. Contribu-tions to Mineralogy and Petrology, 156, 27-48.

Glodny, J., Kûhn, A., 17. Austrheim, H. 2008. Diffusion versus recrys-tallization processes in Rb-Sr geochronology: Isotopic relicts in eclogite facies rocks, Western Gneiss Region, Norway. Geochimica et Cosmochimica Acta, 72, 506-525.

Hammer, Ø.18. 2008. Pattern formation: Watch your step. Nature Physics, 4, 265-266.

Hammer, Ø 19. ., Dysthe, D.K ., Lelu, B., Lund, H., Meakin, P., Jamt-veit, B . 2008. Calcite precipitaiton instability under laminar, open-channel flow. Geochim. Cosmochim. Acta, 72, 5009-5021.

Hartz, E.H., Podladchikov, Y.Y.20. 2008. Toasting the jelly sandwich: The effect of shear heating on lithospheric geotherms and strength. Geology, 36, 331–334.

Heine, C., Muller, R.D., Steinberger, B., 21. Torsvik, T.H. 2008. Subsid-ence in intracontinental basins due to dynamic topography. Phys-ics of the Earth and Planetary Interiors, 171, 252-264.

Hopp, J., Trieloff, M., Brey, G.P., Woodland, A.B., 22. Simon, N.S.C., Wijbrans, J.R., Siebel, W., Reitter, E. 2008. 40Ar/39Ar-ages of phlogopite in mantle xenolites from South African kimberlites: Ev-idence for metasomatic mantle impregnation during the Kibaran orogenic cycle. Lithos, 106, 351-364.

Iyer, K., Jamtveit, B., Mathiesen, J., Malthe-Sørenssen, A.23. Feder, J. 2007. Reaction-assisted hierarchical fracturing during serpentini-zation. Earth and Planetary Science Letters, 267, 503-516.

Iyer, K., Austrheim, H., John, T.24. Jamtveit, B. 2008. Serpentini-zation of the oceanic lithosphere and some geochemical conse-quences: Constraints from the Leka Ophiolite Complex, Norway. Chemical Geology, 249, 66-90.

Jamtveit, B., Malthe-Sørenssen, A.25. Kostenko, O. 2008. Reaction enhanced permeability during retrogressive metamorphism. Earth and Planetary Science Letters, 267, 620-627.

Jensen, M.H., Sneppen, K., 26. Angheluta, L. Kolmogorov scaling from random force fields. Europhysics Letters, 84, 10011.

Jeger P., Schmalholz, S.M., 27. Schmid, D.W., Kuhl, E. 2008. Brittle fracture during folding of rocks: A finite element study. Philosop-hical Magazine ,88, 3245 – 3263.

John, T.,28. Klemd, R., Gao, J., Garbe-Schönberg, C.-D. 2008. Trace-element mobilization in slabs due to non steady-state fluid-rock interaction: constraints from an eclogite-facies transport vein in blueschist (Tianshan, China). Lithos, 103, 1-24.

Kaus B.J.P., Gerya T.V., 29. Schmid D.W. 2008. Recent advances in Computational Geodynamics: Theory, Numerics and Applications. Physics of the Earth and Planetary Interiors. Vol. 171. 2-6.

Krotkiewski, M., Dabrowski, M., Podladchikov, Y.Y.30. 2008. Frac-tional Steps methods for transient problems on commodity com-puter architectures. Physics of the Earth and Planetary Interiors, 171, 122-136.

Løvholt, F., Pedersen, G.K., 31. Gisler, G.R., 2008. Oceanic propaga-tion of a potential tsunami from the La Palma Island. Journal of Geophysical Research, 113, C09026, doi:10.1029/2007JC004603.

Mair, K.,32. Abe, S. 2008. 3D numerical simulations of fault gouge evolution during shear: Grain size reduction and strain localiza-tion. Earth and Planetary Science Letters, 274, 72-81.

Mathiesen, J.33. , Jensen, M.H., Bakke, J.Ø.H. 2008. Dimensions, Ma-ximal Growth Sites and Optimization in the Dielectric Breakdown Model. Phys. Review E77, 066203.

Mathiesen, J.34. , Procaccia, I., Regev, I. 2008. Elasticity with arbitra-rily shaped inhomogeneity. Physical Review E 77, 026606.

2008 Production list


Mazzini, A.35. , Ivanov, M.K., Nermoen, A., Bahr, A., Borhmann, G., Svensen, H., Planke, S. 2007. Complex plumbing systems in the near subsurface: geometries of authigenic carbonates from Dolgo-vskoy Mound (Black Sea) constrained by analogue experiments. Marine & Petroleum Geology, 25, 457-472.

Medvedev, S., Hartz, E.H., Podladchikov, Y.Y. 36. 2008. Vertical motions of the fjord regions of central East Greenland: Impact of glacial erosion, deposition, and isostasy. Geology, 36, 539–542.

Montes-Hernandez, Fernandez-Martinez, A., Charlet, L., 37. Renard, F., Scheinost, A., Bueno, M. 2008. Synthesis of a Se

0 calcite com-

posite using hydrothermal carbonation of Ca(OH)_2 coupled to a complex selenocystine fragmentation. Crystal Growth & Design, 8, 2497-2504.

Montes-Hernandez, Fernandez-Martinez, A., Charlet, L., Tisse-38. rand, D., Renard, F. 2008. Textural properties of synthetic nano-calcite produced by hydrothermal carbonation of calcium hydro-xide. Journal of Crystal Growth, 310, 2946-2953.

Perez-Lopez, R., Montes-Hernandez, G., Nieto, J.M., 39. Renard, F., Charlet, L. 2008. Carbonation of alkaline paper mill waste to reduce CO

2 greenhouse gas emissions into the atmosphere. Ap-

plied Geochemistry, 23, 2292-2300.

Pollok, K., Lloyd, G.E., 40. Austrheim, H., Putnis, H. 2008. Complex replacement patterns in garnets from Bergen arc eclogites: A com-bined EBSD and analytical TEM study. Chemie der Erde Geo-chemistry, 68, 177-191.

Polteau S.,41. Ferré, E.C., Planke, S., Neumann, E.-R., Chevallier, L. 2008. How are saucer-shaped sills emplaced? Constraints from the Golden Valley Sill, South Africa. J. Geophys. Res., 113, B12104.

Polteau, S., Mazzini, A., Galland, O., Planke, S.,42. Malthe-Sørens-sen, A. 2008. Saucer-shaped intrusions: occurrences, emplacement and implications. Earth and Planetary Science Letters, 266, 195-204.

Rey, S.S,. 43. Planke, S., Symonds, P.A. 2009. Seismic volcano stra-tigraphy of the Gascoyne Margin, Western Australia. Journal of volcanology and thermal research , 172, 112-131

Rüpke, L44. ., Schmalholz S.M., Schmid, D.W., Podladchikov, Y.Y. 2008. Automated reconstruction of sedimentary basins using two-dimensional thermo-tectono-stratigraphic forward models – tested on the Northern Viking Graben. AAPG Bulletin, 92, 309-326.

Røyne, A.45. , Jamtveit, B., Mathiesen, J., Malthe-Sørenssen, A. 2008. Controls on weathering rates by reaction induced hierarchi-cal fracturing. Earth and Planetary Science Letters, 275, 364-369.

Schmalholz, S.M., 46. Schmid, D.W., Fletcher, R.C. 2008. Evolution of pinch-and-swell structures in a power-law layer. Journal of Structural Geology, 30, 649-663.

Schmid, D.W., Dabrowski, M., Krotkiewski, D.47. 2008. Evolution of large amplitude 3D fold patterns: A FEM sudy. Physics of the Earth and Planetary Interiors, 171, 400-408.

Simon, N. S. C., Neumann, E.-R.,48. Bonadiman, C., Coltorti, M., Delpech, G., Grégoire, M., Widom, E. 2008. Ultra-refractory do-mains in the oceanic mantle lithosphere sampled as mantle xeno-liths at ocean islands. Journal of Petrology, 49, 1223-1251.

Simon, N. S. C., Podladchikov, Y. Y.49. 2008. The effect of mantle composition on density in the extending lithosphere. Earth and Planetary Science Letters, 272, 148-157.

Steinberger, B., 50. Torsvik, T.H. 2008. Absoolute plate motions and true polar wander in the absence of hotspot tracs. Nature, 452, 620-624.

Svensen, H 51. ., Bebout, G., Kronz, A., Li, L., Planke, S ., Chevallier, L., Jamtveit, B. 2008. Nitrogen geochemistry as a tracer of fluid flow in a hydrothermal vent complex in the Karoo Basin, South Africa. Geochim. Cosmochim. Acta, 72, 4929-4947.

Torsvik, T.H.52. , Müller, R.D., Van der Voo, R., Steinberger, B., Gaina, C. 2008. Global Plate Motion Frames: Toward a unified model. Reviews of Geophysics, 46, RG3004/2008.

Torsvik, T.H.,53. Smethurst, M.A., Burke, K., Steinberger, B. 2008. Long term stability in Deep Mantle structure: Evidence from the ca. 300 Ma Skagerrak-Centered Large Igneous Province (the SCLIP). Earth Planetary Science Letters, 267, 444-452.

Torsvik, T.H.54. , Steinberger, B., Cocks, L.R.M., Burke, K. 2008. Lo-nitude: Linking ancient surface to its deep iterior. Earth and Plan-etary Science letters, 276, 273-282.

Van der Straaten, F., Schenk, V., 55. John, T., Gao, J. 2008. Blueschiest-facies redydration of eclogites (Tian Shan, NW-China): Implica-tions for fluid-rock interaction in the subduction channel. Chemi-cal Geology, 255, 195-219.

Voisin, C., Grasso, J.-R., Larose, E., 56. Renard, F. 2008. Evolution of seismic signals and slip papttern along subduction zones: Insights from a friction lab scale. Geophys. Res. Lett., 35, L08302.

Vrijmoed, J. C.,57. Smith, D. C., Van Roermund, H. L. M. 2008. Ra-man Confirmation of Microdiamond in the Svartberget Fe-Ti type garnet peridotite, Western Gneiss Region, Western Norway. Terra Nova, 20, 295-301.

Zhijie Xu, 58. Meakin, P. 2008. Phase-field modeling of solute precipi-tation and dissolution. Journal of Chemical Physics, 129, 014705.

Publications 2009 and in pressAngheluta, E. Jettestuen, Mathiesen, J.1. 2009. Thermodynamics and roughening of solid-solid interfaces”, Physical Review E (ac-cepted).

Austrheim, H., Corfu, F.2. 2009. Formation of planar deformation features (PDFs) in zircon during coseismic faulting and an evalu-ation of potential effects on U-Pb systematics. Chemical Geology doi:10.1016/j.chemgeo.2008.09.012.

Bahr, A., Pape, T., Bohrmann, G., 3. Mazzini, A., Haeckel, M., Reitz, A., Ivanov, M. 2009. Authigenic carbonate precipitates from the NE Black Sea: a mineralogical, geochemical, and lipid biomarker study. International Journal of Earth Sciences, 98, 677-695.

Bjørk, T.E., Mair, K. Austrheim,H.4. 2009. Quantifying granular ma-terial and deformation: Advantages of combining grain size, shape, and mineral phase recognition analyses. Journal of Structural Ge-ology (accepted).

Bonnetier, E., Misbah, C., 5. Renard, F., Gratier, J.-P., Toussaint, R. 2009. Stability of an elastically stressed rock-fluid interface: effect of the orientation of the main compressive stress, European Phys-ics Journal B, 67, 121-131.

Candela, T., 6. Renard, F., Bouchon, M., Brouste, A., Marsan, D., Schmittbuhl, J., Voisin, C. 2009. Characterization of fault rough-ness at various scales: Implications of three-dimensional high reso-lution topography measurements. Pure and Applied Geophysics (accepted)

de Mahiques, M.M., Wainer, I.K.C., Burone, L., Nagai, R., de Mello 7. e Sousa, S.H., Figueira, R.C.L., da Silveira, I.C.A., Bicego, M.C., Alves, D.P.V., Hammer, Ø. A high-resolution Holocene record on the Southern Brazilian shelf: Paleoenvironmental implications. Quaternary International (in press).


Appendices

Ebner, M., Koehn, D., Toussaint, R., 8. Renard, F. 2009. The influ-ence of rock heterogeneity on the scaling properties of simulated and natural stylolites. Journal of Structural Geology, 31, 72-82.

Engvik, A.K., Golla-Schindler, U., Bernd, J., 9. Austrheim, H., Putnis, A. 2009. Intragranular replacement of chlor-apatite by hydroxy-fluor-apatite during metasomatism. Lithos, accepted.

Fletcher, R.10. 2009. Deformable, rigid, and invicid elliptical inclu-sions in a homogenous incompressible anisotropic viscous fluid. Journal of Structural Geology, doi:10.1016/j.jsg.2009.01.006.

Frehner, M., Schmalholz, S.M., 11. Podladchikov, Y.Y. 2009. Spectral modification of seismic waves propagating through solids exhibit-ing a resonance frequency. Geophys. J. Int., 176, 589-600.

Galland, O., Planke, S., Neumann, E.-R., Malthe-Sørenssen , 12. A. 2009. Experimental modelling of shallow magma emplacement: Application to saucer-shaped intrusions. Earth and Planetary Sci-ence Letters, 277, 373-383.

Gisler, G.,13. 2009. Simulations of the Explosive Eruption of Super-heated Fluids through Deformable Media. Marine & Petroleum Geology, in press.

Gratier, J.-P., Guiguet, R., 14. Renard, F., Jenatton, L., Bernard, D. 2009. A pressure solution creep law for quartz from in-dentation experiments, Journal of Geophysical Research, 114, doi:10.1029/2008JB005652.

Gregory, L.C., Meert, J.G., Bingen, B., 15. Torsvik, T.H., Pandit, M. 2009. Paleomagnetism and geochronology of the Malani Igne-ous Suite, Northwest India: Implications for the configuration of Rodinia and the assembly of Gondwana. Precambrian Research, (in press).

Hammer, Ø. 16. 2009. New statistical methods for detecting point alignments. Computers & Geosciences, doi: 10.1016/j.cageo.2008.03.012.

Hammer, Ø, Dysthe, D.K., Jamtveit, B. 17. 2009.Travertine terracing: patterns and mechanisms. In: Tufas and Speleothems: Unravelling the Microbial and Physical Controls. Geological Society of London Special Publications (accepted).

Iyer, K., Podladchikov, Y.Y.18. 2009. Transformation-induced joint-ing as a gauge for interfacial slip and rock strength. Earth and Planetary Science Letters (in press).

Jamtveit, B19. ., Putnis, C., Malthe-Sørenssen, A. 2009. Reaction in-duced fracturing during replacement processes, Contributions to Mineralogy and Petrology, 157:127-133.

John, T., Medvedev, S., Rüpke, L., Andersen, T.B., Podladchikov, 20. Y.Y., Austrheim, H.O. 2009 Generation of intermediate-depth earthquakes by self-localizing thermal runaway. Nature Geosci-ence, 2, 137-140.

Lisker, F., John, T. 2008. How much denudation at the Ghana 21. transform margin? - A review of the offshore apatite fission track record. Earth Surface Processes and Landforms (Accepted).

Marques F.O., 22. Podladchikov, Y.Y. 2009. A thin elastic core can control large-scale patterns of lithosphere shortening. Earth and Planetary Science Letters, 297, 80-85.

Mazzini, A., Nermoen, A., Krotkiewski, M., Podladchikov, Y.Y., 23. Planke, S., Svensen, H. 2009. Fault shearing as a mechanism for overpressure release and trigger for piercement structures. Implica-tions for the Lusi mud volcano, Indonesia. Marine and petroleum Geology (accepted).

Mazzini, A., Svensen, H., Planke, S,24. Guliyev, I., Akhmanov, G.G., Fallik, T., Banks, D. 2009. When mudvolcanoes sleep: Insight from seep geochemistry at the Dashgil mud volcano, Azerbaijan. Marine and Petroleum Geology, doi:10.1016/j.marpetgeo.2008.11.003.

Meakin, P.,25. Tartakovsky, A. 2009. Modeling and simulation of pore scale multiphase fluid flow and reactive transport in fractured and porous media. Reviews of Geophysics (in press).

Milke, R., Abart, R., Kunze, K., Koch-Muller, M., 26. Schmid, D.W., Ul-mer, P. 2009. Matrix rheology effects on reaction rim growth I: evidence from orthopyroxene rim growth experiments. Earth and Planetary Science Letters, (accepted).

Montes-Hernandez, G., Concha-Lozano, N., 27. Renard, F., Quiri-co, E. 2009. Removal of oxyanions from synthetic wastewater via carbonation process of calcium hydroxide: fundamentals and applications, Journal of Hazardous Materials, doi:10.1016/j.jhazmat.2008.11,120.

Montes-Hernandez, G., Pérez-López, R., 28. Renard, F., Nieto, J. M., Charlet, L. 2009. Mineral sequestration of CO2 by aqueous car-bonation of coal combustion fly-ash. Journal of Hazardous Materi-als, 161, 1347-1354.

Neumann, E.-R., Simon, N.S.C.29. 2009. Ultra-refractory mantle xe-noliths from ocean islands: how do they compare to peridotites retrieved from oceanic sub-arc mantle? Lithos Special Volume, doi:10.1016/j.lithos.2008.06.003.

Pérez-López, R., Montes-Hernandez, G., Nieto, J. M., 30. Renard, F., Charlet, L. 2009. Application of alkaline paper mill waste to re-duce CO2 greenhouse gas emissions into the atmosphere. Applied Geochemistry, /doi 10.1016/j.apgeochem.2008.04.016.

Quintal, B., Schmalholz, S.M., 31. Podladchikov, Y.Y. 2009. Low-fre-quency reflections from a thin layer with high attenuation caused by interlayer flow. Geophysics. In press.

Rozhko, A.Y. 32. 2009. Benchmark for poroelastic and thermoelas-tic numerical orders. Physics of the Earth and Planetary Interiors. doi:10.10.16/j.pepi.2008.08.016.

Sassier C., Leloup, P. H., Rubatto, D., 33. Galland, O., Yue, Y., Lin , D. 2009. Direct measurement of strain rates in ductile shear zones: A new method based on syntectonic dikes, J. Geophys. Res., 114, B01406, doi:10.1029/2008JB005597. [Abstract +Article]

Schmid, D.W.34. , Abart, R., Podladchikov, Y.Y., Milke, R. 2009. Ma-trix rheology effects on reaction rim growth II: coupled diffusion and creep model. Journal of Metamorphic Geology, 27, 83-91.

Schmidt, A., Weyer, S., 35. John, T., Brey, G.P. 2009. HFSE systemat-ics of rutiles and MORB-type eclogites during subduction: some insights into Earth’s HFSE budget. Geochimica et Cosmochimica Acta, 73, 83-91.

Skinner, J., 36. Mazzini, A. 2009. Martian mud volcanism: Terrestrial analogs and implications for formational scenarios. Marine and petroleum Geology (accepted).

Svensen, H., Planke, S., Polozov, A.,37. Schmidbauer, N., Corfu, F., Podladschikov, Y., Jamtveit, B. 2009. Siberian gas venting and the end-Permian environmental crisis. Earth and Planetary Science Letters, 277, 490-500.

Voisin, C., Grasso, J.-R., Larose, E., 38. Renard, F. 2009. Seismic sig-nals and slip patterns down dip subduction zones: insights from a lab scale experiment. Geophysical Research Letters, 35, L08302, doi:10.1029/2008GL033356/.

Webb, K.E., Hammer, Ø.,39. Lepland, A., Gray, J.S. 2009. Pockmarks in the Inner Oslofjord, Norway. Geo-Marine Letters DOI 10.1007/s00367-008-0127-1.


In books and proceedingsAkhmetzhanov, A.M., Kenyon, N.H., Ivanov, M.K., Westbrook, 1. G., Mazzini, A. (Editors), 2008. Deep-water depositional systems and cold seeps of the Western Mediterranean, Gulf of Cadiz and Norwegian continental margins. IOC Technical Series No. 76, UNESCO, 91 pp.

Andersen, H.B., Austrheim, H.O.2. 2008. The Caledonian infra-structure in the Fjord-region of Western Norway; With special em-phasis on the formation and exhumation of high- and ultrahigh-pressure rocks, late- ot post-orogenic tectonic processes and basin formation. Excursion guide, 88 pp. 33 IGC excursion NO 29. Au-gust 15-22 2008.

Cronin, B., Çelik, H., Hurst, A., Gul, M., Gürbüz, K., 3. Mazzini, A., Overstolz, M. 2008. Slope-channel Complex Fill and Overbank Architecture, Tinker Channel, Kirkgecit Formation, Turkey. In: T.H. Nilsen, R.D. Shew, G.S. Steffens and J.R.J. Studlick (Editors), Atlas of Deep-Water Outcrops. AAPG Studies in Geology 56, pp. 363-367.

Røyne, A4. . Cool Photovoltaics: An experimental study of cool-ing devices for densely packed photovoltaic arrays under high concentration. VDM Verlag. ( Dr. Müller, Ed). 2008 (ISBN 978-3836480314) 136 p.

Torsvik, T.H.,5. Gaina, C., Redfield, T.F. 2008. Antarctica and Global Paleogeography: From Rodinia, through Gondwanaland and Pan-gea, to the birth of the Southern Ocean and the opening of gate-ways. In: Cooper, A.K., Barret, P.J., Stagg, H., Storey, B., Stump, E., Wise, W and the 10th ISAES editorial team (eds): Antarctica: A keystone in a Changing World. Proseedings of the 10th interna-tional symposium on Antarcic Earth Sciences. Washington DC: The National Academies Press. doi: 10.3133/of2++7-1047.kp11.

In books and proceedings 2009 and in pressBahr, A., Pape, T., Bohrmann, G., 1. Mazzini, A., Haeckel, M., Reitz, A., Ivanov, M. 2008. Authigenic carbonate precipitates from the NE Black Sea: a mineralogical, geochemical and lipid biomarker study. International Journal of Earth Sciences. (in press).

Gisler, G.2. 2009. Tsunami generation - other sources, chapter 6 in The Sea: Volume 15, Tsunamis, edited by Alan Robinson and Ed-die Bernard pp 179-200.

Gisler, G.R.,3. Weaver, R.P., Gittings, M.L. 2009. Oblique impacts into volatile sediments: ejection distribution patterns, PARA 08 Conference Proceedings, Trondheim, in press.

Torsvik, T.H.4. , Cocks, L.R.M. The Lower Palaeozoic palaeogeo-graphical evolution of the Norteastern and Eastern peri-Gond-wana margin from Turkey to New Zealand. J. Geol. Soc. London Special Publication (in press).

Invited talks 2008 Aarnes, I.1. Magmatic differentiation by fractional crystallization – A scientific journey to Africa and back again. Birthday seminar for Else Ragnhild Neumann. The Academy of Science, Oslo. 28.11.08 .

Austrheim, H.2. Zircon coronas around ilmenite – a key to under-stand the metasomatic and ore forming processes in the Kongsberg-Bamble sectors. Birthday seminar for Else Ragnhild Neumann. The Academy of Science, Oslo. 28.11.08.

Austrheim, H.3. CO2 sequestration and extreme Mg-leaching in ser-pentinized peridotite clasts of sediementray basins. Natural His-tory Museum Oslo 12 February.

Feder, J.4. Self-Affine Dynamics of Stick-Slip Friction. ETH. 28. January 2008.

Feder, J.5. Structural Phase Transitions in Perovskites, Florida State University, February 18 2008.

Feder, J.6. Self-Affine Dynamics of Stick Slip Friction, Florida State University, February 27 2008.

Feder, J.7. Two Phase Flow in Porous and Geological Media, Ecole Polytechnique, June 26 2008.

Feder, J.8. Dispersion at high and low Peclet numbers, Workshop on Flow in Porous Media, Brasília, October 20th - 24th, 2008.

Feder, J.9. Extrusion: Plastic Deformation & Friction, Invited pre-sentation Norsk Hydro, June 18 2008

Fletcher, R. 10. Grain-scale and macroscopic stress evolution in ex-huming rock: fracturing and weathering. The 21 Kongsberg semi-nar 7-9 May 2008. (Invited talk).

Gisler, R.G.11. Oblique Impacts into Volatile Sediments: Ejection Distribution Patterns. The 21 Kongsberg seminar 7-9 May 2008. (Invited talk).

Galen R.G.12. Hydrocode calculations of the generation of tsuna-mis by landslides with application to La Palma and Åknes, invited seminar at National Oceanographic Centre, Southampton UK; 7 Feb 2008.

Galen R. G.13. Asteroid impacts, tsunamis, and mud volcanos: simu-lating violent processes in geophysics, invited seminar at Simula Research Laboratory, Oslo; 29 Feb 2008.

Galen R. G.14. R. Weaver, M. Gittings, Oblique impacts into volatile sediments: ejection distribution patterns, invited talk at the PARA ‘08 Meeting, Trondheim; 13-15 May 2008.

Galen R. G.15. Generation scenarios for Atlantic-region tsunamis: landslides and volcanos, invited talk at the AGU San Francisco; 15-19 Dec 2008.

Jamtveit, B.16. Reaction assisted fluid migration through rocks. Uni-versity of München, 25th Jan 2008.

Jamtveit, B.17. Hydration of the Earth’s crust: The role of reaction driven fragmentation. University of Münster, 5th June 2008.

Jamtveit, B.18. Malthe-Sørenssen, A. Stress generation and hierarchi-cal fracturing in reactive rocks. The 21 Kongsberg seminar 7-9 May 2008.

Jøssang, T., Feder, J19. . Drainage in 2d Systems; Experiments and simulations. Workshop on Flow in Porous Media, Brasília, Octo-ber 20th - 24th, 2008.

Mathiesen, J.20. Solid-solid phase transformation and the roughening of stylolites. The 27th IUGG Conference on Mathematical Geo-physics, June 15-20, 2008, Spitsbergen.

Mathiesen, J.21. Morphology studies of desiccation patterns and hi-erarchical fracture networks. The 21 Kongsberg seminar 7-9 May 2008.

Mathiesen, J.22. Competition between size diffusion and fragmenta-tion: a case study of crystal formation in the Greenland North-GRIP ice core”. ESF – Workshop on Modelling and interpretation of ice microstructurs”; Goettingen, April 7. – 12. 2008.

Mathiesen, J.23. Collaboration on Thermo Haline circulation. Niels Bohr Institute, Cophenhagen, DK; April 22. – 26., 2008.

Mazzini. A.24. Causes and triggers of the LUSI Mud Volcano, Indo-nesia. Invited speaker at the Dutch Petroleum Geological Society, The Hague.


Appendices

Mazzini. A.25. Causes and triggers of the LUSI Mud Volcano, Indo-nesia. Invited speaker at the Wintershall oil company. The Hague

Mazzini, A., Svensen, H., Planke, S.,26. Akhmanov, 2008. Causes and triggers of the LUSI Mud Volcano, Indonesia. In: ”Subsour-face sediment remobilization and fluid flow in sedimentary basins”, 21-22 October, London, UK.

Mazzini, A., Svensen, H., Planke, S.,27. Akhmanov, 2008. New expe-riments on LUSI Mud Volcano, Indonesia. LUSI crisis workshop. 27 February, Surabaja, Indonesia.

Medvedev S., Hartz E.H., Podladchikov Y. Y., Souche A. 28. Verti-cal motions of the fjord regions of central East Greenland: Impact of glacial erosion, deposition, and isostasy. Workshop in Aarhus, Denmark, 11-12 December, 2008.

Meakin, P.29. Fracture models. The 21 Kongsberg seminar 7-9 May 2008.

Neumann, E.-R., Simon, N.S.C.30. Ultra-refractory mantle in the oceanic domain. 33IGC, Oslo, 6 14 August. (Keynote talk).

Planke, S.31. The Golden Valley. Birthday seminar for Else Ragnhild Neumann. The Academy of Science, Oslo. 28.11.08.

Raufaste, C., Santucci S.32. How do the materials flow or break? French Cultural Center, Oslo, 15-10-2008.

Renard, F.,33. Bernard, D. Imaging of a rupture path by X-ray micro-tomography when hydro-fracturing a porous limestone.

Santucci, S.34. Crackling Dynamics during material failure. HUT, Helsinki, Finland; April 16.-19. 2008.

Santucci, S. 35. Quake catalogs at the laboratory scale. The 21 Kongs-berg seminar 7-9 May 2008.

Simon, N.S.C.36. Mantle phase transitions during rifting. EGU, Vi-enna, Austria, April 13 – 19 2008.

Simon, N.S.C.37. The composition of the mantle lithosphere and how to make it. Birthday seminar for Else Ragnhild Neumann. The Aca-demy of Science, Oslo. 28.11.08.

Svensen, H.38. New perspectives on large ignons provinces and en-vironmental crises; University Joseph Fourier, Grenoble, France; January 5 – 8.

Svensen, H.39. Global environmental crises caused by sill emplace-ment and contact metamorphism in sedimentary basins. PetroBras, Rio de Janeiro, 26 March 2008.

Svensen, H.40. Sill emplacement and contact metamorphism in the Vøring Basin during formation of the North Atlantic Volcanic Pro-vince and the implications for the PETM climate change. Keynote lecture, The 33rd International Geological Congress, Session on the evolution of the NE Atlantic, Oslo, 7. August 2008.

Svensen, H.41. Sill emplacement, contact metamorphism, and gas venting in the Vøring Basin during formation of the North Atlan-tic Volcanic Province and the implications for the PETM climate change. Keynote lecture, Subsurface remobilization and fluid flow in sedimentary basins, Geol Soc London, October 20, 2008.

Treagus, S.H., 42. Fletcher, R.C. Controls on folding on different scales in multilayered rocks. Geological Society of America 2008 Annual Meeting.

Torsvik, T. 43. Fragmentation of continents. The 21 Kongsberg semi-nar 7-9 May 2008.

Torsvik, T. 44. Oslo Hot Spot. Birthday seminar for Else Ragnhild Neumann. The Academy of Science, Oslo. 28.11.08.

Vrijmoed, J. C.45. Physical and chemical interaction in the interior of the former Caledonian mountains of Norway. The Faculty of Earth and Life Sciences, Vrije Universiteit Amsterdam, 18 Decem-ber 2008.

Yarushina V.M.46. Fluid flow in viscoplastic porous media: porosity waves as a mechanism for fluid expulsion. Harvard University, De-partment of Earth and Planetary Sciences and School of Engineer-ing and Applied Sciences.

Yarushina V.M.47. Low-frequency seismic wave attenuation due to microplasticity in porous media. Boston University, Department of Earth Sciences.

Yarushina V.M. 48. Compaction Driven Fluid Flow in Viscoplastic Po-rous Media:Porosity Waves as a Mechanism for Fluid Expulsion. Yale University, Department of Geology and Geophysics.

Talks and posters at conferences 2008

Aarnes, I., Podladchikov, Y.Y., Neumann, E.-R.1. Post-emplace-ment melt-flow induced by thermal stresses as a feasible mecha-nism for reversed differentiation in tholeiitic sills. LASI III; 2008-09-14 - 2008-09-18 (Poster).

Aarnes, I., Podladchikov, Y.Y., Neumann, E.-R. 2. Post-emplacement melt-flow induced by thermal stresses as a feasible mechanism for reversed differentiation in tholeiitic sills. 33rd International Geo-logical Congress; 2008-08-06 - 2008-08-14 (Poster).

Aarnes, I., Podladtchikov, Y.Y., Neumann, E.-R. 3. Post-emplace-ment melt flow as possible differentiation mechanism in sills. Dave Yuen’s international 60-birthday symposium; 2008-06-13 - 2008-06-14 (Poster).

Aarnes, I., Svensen, H.4. Gas formation in contact aureoles: Con-straints from kinetic and thermal modeling. LASI III. International conference, Elba 14-18 September (Talk).

Aarnes, I., Svensen, H. Polteau, S.5. Gas formation from black shale during contact metamorphism. 33rd International Geologi-cal Congress; 2008-08-06 - 2008-08-14 (Talk).

Abe, S6. ., Mair, K. How do Things break in Fault Gouge? Abra-sion vs. grain splitting in Discrete Element Simulations. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Andersen, T.B. 7. Inside intermediate and deep earthquakes: What can we learn from field studies? (combined with modeling). Goldschmidt lecture NGU Trondheim; 2008-10-10 - 2008-10-10 (Talk).

Andersen, T.B., Austrheim, H.O., John, T., Medvedev, S. 8. Geol-ogy of intermediate to deep earthquakes. Norsk geologisk forening, avdeling Tromsø; 2008-03-07 - 2008-03-07 (Talk).

Andersen, T.B., Austrheim, H.O., John, T., Medvedev, S., Mair, 9. K., Podladchikov, YY. Geology of intermediate-deep earthquakes and the strength of rocks at high confining pressure. International Geological Congress no 33, Oslo Norway 2008-08-06 - 2008-08-14 (Talk).

Andersen, T.B., Mair, K., Austrheim, H.O., Podladchikov, Y.Y., 10. Vrijmoed, J.C. The strength of upper mantle peridotite determined from ultramafic pseudotachylytes. The Kongsberg seminar 7-9 May 2008 (Poster).

Andersen, T.B., Mair, K., Austrheim, H.O., Podladchikov, Y.Y., 11. Vrijmoed, J.C. The strength of upper mantle peridotite determined from ultramafic pseudotachylytes. 21st Kongsberg seminar; 2008-05-07 - 2008-05-09 (Poster).


Andersen, T.B., Marques, F.O., Schmid, D.W., 12. Geological and modeling constraints on exhumation across the Nordfjord-Sogn Detachment Zone, Western Norway. International Geological Congress no 33; 2008-08-06 - 2008-08-14 (Talk)

Angheluta, L.13. Interface instability driven by a solid-solid phase transformation, Dynamics Days Delft, 25-29 August 2008 (Talk).

Angheluta, L. 14. Roughening of a solid-solid interface: Stability anal-ysis”, Oscarborg student conference 3-4 March 2008 Talk).

Angheluta, L. 15. Interface instability driven by a solid-solid phase transformation. Dynamics Days Delft, August 2008 Talk).

Angheluta, L., Jettestuen, E., Mathiesen, J.16. Interface instability driven by a solid-solid phase transformation: Roughening of stylo-lites. The Kongsberg seminar 7-9 May 2008 (Poster).

Angheluta, L., Jettestuen, E., Mathiesen, J.17. The thermodynamics and roughening of solid-solid interfaces, 2008 AGU Fall Meeting (Poster).

Austrheim, H. et al.18. Fragmentation of olivine and hydration of the oceanic lithosphere by seismic pumping. The Kongsberg seminar 7-9 May 2008 (Poster).

Bachaud, P., Berne, P., Leclerc, J.P., 19. Renard, F. Determination of the petrophysical characteristics of caprock samples for carbon di-oxide storage in deep saline aquifers. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Bachaud, P., Berne, P., 20. Renard, F., Sardin, M., and Leclerc, J.-P. (2008). Using tracer experiments to determine deep saline aquifers caprocks characteristics for carbon dioxide storage, 5^th Interna-tional Conference on /Tracers and Tracing Methods/ , 2-6 Septem-ber 2008, Tiradentes, Brasil. (Talk).

Beuchert, M.J. & Podladchikov, Y.Y21. . “Viscoelastic modeling of mantle convection”. Interdisciplinary Constraints on Solid Earth Dynamics from the Crust to the Core, Dave Yuen’s 60

th Birthday

Symposium, Elm, Switzerland, 12-14 june 2008 (Poster).

Beuchert, M.J., Podladchikov, Y.Y. & Simon, N.S.C..22. Stability of the Large Low Shear Velocity Provinces (LLSVPs) in the lower mantle. 33rd International Geological Congress, Oslo, Norway, 06-14 au-gust 2008 (Talk).

Beuchert, M.J., Podladchikov Y.Y., Simon, N.S.C.23. Numerical in-vestigation of the dynamics of the equatorial Large Low Velocity Provinces in the Earth’s deep mantle. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Beuchert, M.J., Podladchikov, Y.Y., Simon, N.S.C., 24. Rüpke, L.H. Viscoelastic modeling of craton stability. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Beuchert, M.J., Podladchikov, Y.Y.,25. Simon, N.S.C., Rüpke, L.H. (2008). Viscoelastic modeling of craton stability. Geophys. Res. Abstr., 10: A-09178.

Beuchert, M.J., Simon, N.S.C., Podladchikov Y.Y.26. Phase Transi-tions and Thickness of the Oceanic Lithosphere. European Geo-science Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Bjørk, T.E., K. Mair, H. Austrheim.27. Quantifying granular material and deformation: Advantages of combining grain size, shape, and mineral phase recognition analyses. The Kongsberg seminar 7-9 May 2008 (Poster).

Bjørk, T.E., Mair, K., Austrheim, H.28. Quantifying fault rocks and deformation: Advantages of combining grain size, shape, and min-eral phase recognition analyses.European Geoscience Union Gen-eral Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Brantley, S., 29. Fletcher, R.C. Relationship between corestone size, weathering rate, and erosion for a steady state model applied to natural systems. Goldschmidt conference 2008(Talk).

Candela, T., 30. Renard, F., Schmittbuhl, J., Bouchon, M. Roughness of fault surfaces: implications of high resolution topography mea-surements at various scales. European Geoscience Union General Assembly. Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Croizé, D., Bjørlykke, K.,31. Renard, F., Dysthe, D.K., Jahren, J. Pres-sure-solution in carbonate - An experimental study,. IGC 2008; 2008-08-06 - 2008-08-14 (Poster).

Croizé, D., Bjørlykke, K., 32. Dysthe, D.K., Renard, F., Jahren, J. De-formation of carbonates, experimental mechanical and chemical compaction. European Geoscience Union General Assembly Vi-enna, Austria, 13.4. - 18.4. 2008 (Poster).

Dabrowski M., Schmid D.W.,33. Mechanical Anisotropy of a Two-Phase Composite Consisting of Aligned Elliptical Inclusions. Yors-get 1-3 July 2008, Oviedo, Spain. (Talk).

Dabrowski, M. Schmid, D.W.34. Numerical study of a rigid circular inclusion in an anisotropic matrix. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Dabrowski, M., Hartz, E.H.; Podladchikov, Y. Y.35. Migmatization induced overpressure, East Greenland case study. European Geo-science Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Dabrowski, M., Schmid, D.W.; Krotkiewski, M.M.36. Evolution of large amplitude 3D fold patterns: a FEM study. European Geosci-ence Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Dabrowski, M., Schmid, D.W., Podladchikov, Y.Y.37. Two-Phase Composite Subject to Large Deformation: Shape and Mechanical Anisotropy Development. The Kongsberg seminar 7-9 May 2008 (Poster).

Ebner, M., Koehn, D., Toussaint, R., 38. Renard, F., Schmittbuhl, J. Scaling behavior of natural and simulated stylolites. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Fletcher, R.C.39. Wavelength selection in 3-D decollement folds of the appalachian Plateau Province with estimates of rheological pa-rameters. Geological Society of America 2008 Annual Meeting

Eriksen, O.K. Dysthe, D.K.40. An experimental study of stylolite for-mation. The Kongsberg seminar 7-9 May 2008 (Poster).

Fristad41. , K., Svensen, H., Planke, S., Polozov, A.G. Geochemis-try of end-permian crater lake sediments in the tunguska basin, siberia, and the implications for extinction mechanisms. AGU Fall meeting 15.12-19.12.2008 (Poster).

Gac, S., Huismans, R., 42. Simon, N.S.C., Semprich, J., Podladchikov, Y.Y. (2008). Are phase changes at the origin of the large subsidence of Barents sea basins? Insights from dynamic numerical modeling. IGC Abstr. STT02709L.

Galerne, C.Y., Neumann, E.-R., Aarnes I., Planke S.43. Post-em-placement melt flow in saucer-shaped sills: a mechanism for the generation of I-, D- and S-shaped compositional profiles. LASI III Conference, Elba Island -15-18 September 2008 (Talk).

Galerne, C.Y., Neumann, E.-R., Planke, S.44. 2008. Insights on the emplacement of saucer-shaped sill complexes from large-scale geochemical architecture: example of the Golden Valley Sill Com-plex, South Africa, (Talk), 33

rdIGC, Oslo.

Galerne, C.Y., Galland, O., Neumann, E.-N., Planke, S.45. 2008. What are the feeders of sills? Insights from field observations, geo-chemistry and experimental modeling, 33

rdIGC, Oslo (Poster).


Appendices

Galerne, C.Y., Tantserev, E., Podladchikov, Y.Y., Neumann. E.-R.46. 2008. Modeling of porous reactive flow in cooling igneous sills: the role of near solidus melt segregation in magmatic differentiation, EGU General Assembly, Vienna. (Talk).

Galerne, C.Y., Neumann, E.-R., Aarnes, I.47. 2008. Post-emplace-ment melt flow in saucer-shaped sills: a mechanism for the genera-tion of S-, D-, and I-shaped compositional profiles, EGU General Assembly, Vienna (Poster),

Galland, O, S. Planke, A. Malthe-Sørenssen, E.-R. Neumann48. . Mechanical coupling between magma intrusion and deformation of country rock: application to dynamic emplacement of saucer-shaped sills. The Kongsberg seminar 7-9 May 2008 (Poster).

Gisler, G.49. Generation of non-earthquake tsunamis, AGU San Francisco; 15-19 Dec 2008 (Talk)

Gisler, G., Mair, K.50. Effect of water depth on efficiency of cratering in crystalline rock with application to the Gardnos impact cra-ter, International Geological Conference, Lillestrøm; August 6 -14 2008 (Poster).

Gisler, G., 51. Svensen, H., Mazzini, A., Polteau, S., Galland, O., Planke, S. Simulations of the explosive eruption of supercriti-cal fluids through porous media, EGU Vienna; 13-18 April 2008 (Poster).

Gisler, G.,52. Tsikalas, F. Insights into gravitational collapse and resurge infilling on marine sedimentary-target impact craters re-vealed by refined numerical simulations of the Mjølnir Crater, In-ternational Geological Conference, Lillestrøm; August 6 -14 2008 (Talk)

Gisler, G.,53. , Weaver, R., Gittings, M. Oblique impacts into volatile sediments: ejection distribution patterns, International Geological Conference, Lillestrøm; August 6 -14 2008 (Talk).

Gratier, J.-P., 54. Renard, F., Boullier, A.-M. Evidence of pressure solu-tion processes in the SAFOD 2 samples. EUROPEAN GEOSCI-ENCE UNION GENERAL ASSEMBLY Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Hammer, Ø., Webb, K.E.55. Deflection of oceanic currents in pock-marks. The Kongsberg seminar 7-9 May 2008 (Poster).

Huang, H, 56. Meakin, P., Malthe-Sorenssen, A., Wood, T. Palmer C., nd Earl Mattson, Modeling deformation & fracturing of oil shale rock induced by in situ fluid generation, Oil Shale 2008, Colorado School of Mines, October 13-15, 2008 (Oral).

Huismans, R., 57. Planke, S., Tsikalas, F., Simon, N., et al. (2008). IODP drilling of conjugate north Atlantic volcanic rifted margins, causes and Implications of excess magmatism. IGC Abstr. SD-D01406L.

Jamtveit, B., Austrheim, H., Raufaste, C., Røyne, A., Malthe-58. Sørenssen, A. Reaction-driven fracturing during replacement pro-cesses and metamorphism. AGU Fall meeting, San Fransisco, 15 December 2008 (Talk).

John, T., Podladchikov, Y.Y.59. Drying porosity waves: add fluids to dry up. The Kongsberg seminar 7-9 May 2008 (Poster).

John, T, Podladchikov, Y.Y., Beinlich, A.,60. Klemd, R. (2008). Dry-ing porosity waves: add fluids to dry up. International Geological Conference no 33. (Talk).

John, T, Podladchikov, Y.Y., Beinlich, A,61. Klemd, R. Drying poros-ity waves: add fluids to dry up. European Geoscience Union Gen-eral Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

John, T., 62. Layne, G., Haase, K. (2008). The chlorine isotopic com-position of mantle endmembers. International Geological Confer-ence no 33. (Talk).

John, T., 63. Layne, G., Haase, K. (2008) The chlorine isotope signa-ture of mantle endmembers. Goldschmidt conference. (Talk).

Kihle, J., Harlov, D., 64. Jamtveit, B., Frigaard, Ø. SiO2-Al2O3 mis-cibility at dry granulite facies conditions revealed by formation of epitaxially exolved quartz inclusions in corundum from a sap-pirine-garnet boudine, Bamble granulite terrane, SE Norway. The 33rd IGC conference, Oslo, 11 August 2008 (Poster)

John, T., Vrijmoed, J.C.,65. van der Straaten, F., Podladchikov, Y.Y., Jamtveit, B. Hydration of eclogite at the slab-wedge interface: an example of fluid infiltration into a swelling system. European Geo-science Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Krotkiewski, M. 66. High performance, large scale computations on unstructured grids, Notur meeting 2008, Tromsø, Norway, 03.06. – 05.06. 2008 (Poster)

Krotkiewski, M., Dabrowski, M., Y.Y. Podladchikov.67. Reactive transport modeling on a modern desktop: resolving versus upscal-ing. The Kongsberg seminar 7-9 May 2008 (Poster).

Krotkiewski, M., Dabrowski, M; Podladchikov, Y.Y.68. High resolu-tion 3D modeling of heterogeneous parabolic and hyperbolic prob-lems on structured meshes. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Krotkiewski, M., Podladchikov, Y.Y.69. Impact of tectonic forces on clay fluidization and creation of mud volcanos. The Kongsberg seminar 7-9 May 2008 (Poster).

Lisker, F.; 70. John, T.; Ventura, B. Denudation and uplift across the Ghana transform margin as indicated by new apatite fission track data. European Geoscience Union General Assembly Vi-enna, Austria, 13.4. - 18.4. 2008 (Poster).

Løberg, M., Podladchikov, Y.Y.71. Compaction-driven fluid flow in chemically reactive porous media. The Kongsberg seminar 7-9 May 2008 (Poster).

Mair, K. 72. Fragmentation in fault zones.The 21 Kongsberg seminar 7-9 May 2008. (Poster).

Mair, K.,73. Abe S., 3D numerical simulations of falt zone evolution: Gouge comminution and strain partitioning. American Geophysi-cal Union Fall Meeting, San Francisco, USA, December 2008. (Poster).

Mazzini, A74. . Causes and Triggers of the Lusi Mud Volcano, Indo-nesia. AAPG International Meeting Cape Town, South Africa (Talk).

Mazzini, A.75. Causes and Triggers of the Lusi Mud Volcano, Indone-sia . The geological society Conference: Subsurface sediment remo-bilization and fluid flow in sedimentary basins, London, UK 19-23 October (Talk).

Mazzini, A.: 76. Causes and Triggers of the Lusi Mud Volcano, Indo-nesia; 2008 AAPG International Meeting Cape Town, South Af-rica; October 25.-November 1, 2008 (Talk).

Mazzini, A., Gisler, G., Krotkiewski, M., Nermoen, A., Podlad-77. chikov, Y.Y., Svensen, H., Planke, S., Akhmanov, G.G. Multidis-ciplinary approach for mud volcano eruptions. European Geosci-ence Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Meakin, P.78. Pore scale modeling and simulation of geosystems, US Department of Energy workshop on Scientific Impacts and Op-portunities for Computing, January 10-13, 2008, Maui, Hawaii. (Oral).

Meakin, P.79. Pore scale simulation of multiphase fluid flow and re-active transport in fractured and porous media.Brown University, Division of Applied Mathematics, May 1 (2008). (Oral).


Meakin, P.80. Research on travertine hot springs at the Center for the Physics of Geological Processes, University of Oslo. National Sci-ence Foundation Chautauqua Workshop, Mammoth Hot Springs, Yellowstone National Park, Wyoming, July 20, 2008. (Oral).

Meakin, P., 81. Huang, H., Malthe-Sørenssen, A. Discrete element fracture models, Kongsberg Seminar: Kongsberg, May 7-9, 2008. (Oral).

Meakin, P.,82. Huang H., Malthe-Sorenssen, A. Coupling between fluid generation, fluid flow, deformation and fracturing in porous media: Discrete element, particle and continuum methods, Ameri-can Geophysical Union Meeting, San Francisco, Dec 17 2008. (Oral).

Meakin, P. 83. Huang, H., Tartakovsky, A., Xu, Z., Li, Z. Pore scale simulation of multiphase fluid flow and reactive transport using particle methods and continuum fluid dynamics, International Conference on Computational Methods in Water Resources, San Francisco, July 8, 2008. (Oral).

’84. Meakin, P., Zhijie X. Dissipative particle dynamics and related methods for multiphase fluid flow in fractured and porous media, 6th International Conference on Computational Fluid Dynamics in the Oil & Gas, Metallurgical and Process Industries, Trondheim, June 10-12, 2008. (Oral).

Medvedev, S.85. Vertical motions of the fjord regions of central East Greenland: Impact of glacial erosion, deposition, and isostasy (In-vited Talk), WORKSHOP: The role of isostasy, climate and erosion for the evolution of North Atlantic topography , Aarhus, Denmark, 11-12 December 2008 (Talk).

Medvedev S, E.H. Hartz, E.H., Podladchikov, Y.Y.86. Vertical mo-tions of the fjord regions of central East Greenland: Impact of gla-cial erosion, deposition, and isostasy. The Kongsberg seminar 7-9 May 2008 (Poster).

Medvedev, S., John, T., Andersen, T.B:, Podladchikov, Y.Y., Aus-87. trheim, H.O. Self-localizing thermal runaway as a mechanism for intermediate depth earthquakes: numerical studies and compari-son with field observations. International Geological Congress no 33; 2008-08-06 - 2008-08-14 (Talk).

Montes-Hernandez, G., Charlet, L., 88. Renard, F. (2008). Growth of a Se-0/calcite composite using hydrothermal carbonation of Ca(OH)(2) coupled to complex selenocystine fragmentation, Goldschmidt Conference, 13-18 July 2008, Vancouver, Canada. (Talk).

Montes-Hernandez, G.,89. Renard, F., Charlet, L. (2008). Ex-situ min-eral sequestration of CO2 by aqueous carbonation of alkaline solid waste, 22^ème RST, 21-24 April 2008, Nancy, France. (Talk).

Montes-Hernandez, G., 90. Renard, F., Charlet, L. (2008). Mineral se-questration of CO_2 and removal of dissolved toxic ions by using aqueous carbonation of lime and/or portlandite, ACEME confer-ence, 1-3 October 2008, Roma, Italy. (Talk).

Nermoen, A., Galland, O., Fristad, F., Podladchikov, Y.Y., Malthe-91. Sørenssen, A. Experimental modelling of piercement structure for-mation in sedimentary basins. European Geoscience Union Gen-eral Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).

Nermoen, A., Mazzini, A., Gisler, G.R., Krotkiewski, M., Podlad-92. chikov, YY., Svensen, H., Planke, S., Akhmanov, G.G. A multi-diciplinary approach for mud volcano eruptions - Lusi. Eurpean Geosciences Union; 2008-04-24 - 2008-04-29

Nermoen, A., O. Galland, K. Fristad, Y. Y. Podladchikov, A. 93. Malthe-Sørenssen, H. Svensen. Experimental constraints on flu-idization for the formation of piercement structures in sedimentary basins. The Kongsberg seminar 7-9 May 2008 (Poster).

Neumann, E.-R., Simon, N.S.C. 94. Ultra-Depleted Domains in the Oceanic Mantle Lithosphere. 33. International Geological Con-gress; 2008-08-06 - 2008-08-14 (Talk).

Neumann, E.-R., Simon,95. N.S.C. (2008). Ultra-refractory mantle in the oceanic domain. IGC Abstr. EID05411L.

Nicolaisen, F., A. Rozhko, A. Malthe-Sørensen, A. Nermoen.96. Simulation of Hydrothermal Vent Complexes. The Kongsberg seminar 7-9 May 2008 (Poster).

Osmundsen, P.T., Andersen, T.B., Braathen, A., Roberts, D., 97. Redfield, T.F. Formation and deformation of the Norwegian `Old Red Sandstone´: an overview. International Geological Congress no 33; 2008-08-06 - 2008-08-14 (Talk).

Polteau, S, Svensen H., Planke S., Aarnes I.98. (2008). Geochemis-try of contact aureoles in the Karoo Basin and the implication for the Toarcian carbon isotope excursion, IGC 2008 (Talk).

Polteau, S, Svensen H., Planke S., Aarnes I.99. (2008), Geochem-istry of contact aureoles in the Karoo Basin and the implication for the Toarcian carbon isotope excursion, IGC 2008. ((Talk, H.Svendsen`s workshop).

Polteau S.,100. E. C. Ferré, S. Planke, E.-R. Neumann (2008). How are saucer-shaped sills emplaced? Constrains from the Golden valley sill, South Africa, IGC 2008 (Talk).

Polteau S., Svensen H., Planke S., Aarnes I.101. (2008), Contact metamorphism and venting in the Karoo Basin, AGU Fall Meet-ing, Elkins-Tanton workshop on the Siberian Traps and Mass Ex-tinction (Talk).

Polteau, S, Svensen H., Planke S., Aarnes I.102. (2008) Contact metamorphism and the global carbon cycle, Eos Trans. AGU, 89(53), Fall Meet. Suppl., Abstract U41B-0018 (Poster).

Raufaste, C.103. , Cheddadi I., Marmottant P., Saramito P., Graner, F. Rheology and imagery of 2D flow of foam: from bubble scale to continuous modeling. Congress of the French Group of Rheol-ogy, Palaiseau, France. 20-22 October 2008. (Poster).

Raufaste, C., D. K. Dysthe, B. Jamtveit, A. Røyne, J. Mathiesen, 104. A. Malthe-Sørenssen. Experimental approaches to replacement processes. The Kongsberg seminar 7-9 May 2008 (Poster).

Renard, F.105. (2008). Disolution-precipitation processes driven by stress gradients in the Earth’s crust, Fourth Marie Curie Summer School /Knowledge Based Materials/ , Trest, Czech Republic, 19-29 August 2008. (Talk).

Renard, F106. ., Le Guen Y., Hellmann, R., and Gratier, J.-P. (2008). Couplages mécano-chimiques et endommagement lors de l’injection de CO_2 , Journée du Comité Français de Méca-nique des Roches, 23 Octobre 2008. (Talk).

Renard, F., K. Mair.107. Fragmentation, gouge production, and sur-face roughness evolution on experimentally simulated faults. The Kongsberg seminar 7-9 May 2008 (Poster).

Rüpke, L., 108. Schmid, D., Podladchikov, Y.Y., Schmalholz, Auto-mated thermo-tectono-stratigraphic basin reconstruction - Ex-amples from the Norwegian Sea and North Sea, American As-sociation of Petroleum Geologists, San Antonio (Talk).

Rüpke, L.H., 109. Schmid, D.W., Schmalholz, S. M., Podladchikov, Y.Y. Integrated basin modeling - linking lithosphere and sedi-mentary basin processes. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Røyne, A., D.K. Dysthe, J. Bisschop.110. Subcritical cracking in cal-cite single crystals. The Kongsberg seminar 7-9 May 2008 (Post-er).


Appendices

Røyne, A., Dysthe, D.K., Bisschop,111. J., Mechanisms of subcriti-cal cracking in calcite. AGU Fall meeting 15.12. – 19.12.2008 (Poster)

Sarwar, M., Santucci, S., Dysthe, D.K., Mair, K.112. Energy dissipa-tion in a simulated fault system. The Kongsberg seminar 7-9 May 2008 (Poster).

Schmid, D., Dabrowski, M., Krotkiewski, M.113. 3d folding. Inter-national Geological Congress Oslo, Norway (Talk).

Schmid, D.W.114. ; Abart, R.; Podladchikov, Y.Y.; Milke, R. Matrix rheology effects on reaction rim growth: coupled diffusion and creep model. European Geoscience Union General Assembly Vi-enna, Austria, 13.4. - 18.4. 2008 (Talk).

Semprich J., et al.115. Evaluation of phase transitions in the lower crust as mechanism for basin formation. The Kongsberg seminar 7-9 May 2008 (Poster).

Semprich, J., Simon, N. ,Pordladchikov, Y.Y.,116. The effect of pres-sure, temperature and composition on physical rock properties. Goldschmidt conference 13.07 – 18.07.2008 (talk)

Semprich, J., Simon, N., Podladchikov, Y.Y.117. Compression and subsequent phase transitions as a mechanism for basin formation. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).

Semprich, J., Simon, N.S.C., Podladchikov, Y.Y.,118. Gac, S., Huis-mans, R. (2008). Evaluation of phase transitions in the lower crust as mechanism for basin formation. IGC Abstr. MPM11305L.

Simon, N.S.C.119. (2008). Mantle phase transitions during rifting. Geophys. Res. Abstr., 10: A-02115 (solicited).

Simon, N.S.C., Podladchikov, Y.Y.120. (2008). Mantle phase chang-es, partial melting and subsidence during rifting. IGC Abstr. STT02708L.

Souche, A., Medvedev, S., Andersen, T.B.121. Thermal evolution in the hanging-wall of a low angle normal fault: A Finite Element study of the Nordfjord Sogn Detachment zone. 21st Kongsberg seminar; 2008-05-07 - 2008-05-09 (Poster).

Vrijmoed, J. C.,122. Detailed geological mapping of fragmented ul-tra-high pressure rocks at Svartberget, West-Norway. Kongsberg seminar 2008. (Poster)

Vrijmoed, J. C., Podladchikov, Y. Y., Andersen, T.B.,123. Corfu, F., 2008, An alternative model for ultra-high pressure in the Svart-berget olivine-websterite, Western Gneiss Complex, Norway, 33th International Geological Congress, 6-14 August, Oslo, Nor-way. (Talk)

Vrijmoed, J. C., Austrheim, H., John, T., Podladchikov, Y. Y. 124. 2008. Metasomatism of the UHP Svartberget olivine-websterite body in the Western Gneiss Complex, Norway, 33th Internation-al Geological Congress, 6-14 August, Oslo, Norway. (Talk)

Vrijmoed, J. C., Austrheim, H., John, T., Podladchikov, Y. Y.125. 2008. Metasomatism of the UHP Svartberget olivine-websterite body in the Western Gneiss Complex, Norway, Geochimica Et Cosmochimica Acta, 72, A989. (Talk)

Vrijmoed, J. C., Austrheim, H.126. 2008. Implications of metaso-matism for geochronology and P-T estimates: evidence from the Western Gneiss Region (WGR), Norway, Geophysical Research Abstracts, Vol. 10, EGU2008-A-09874. (Talk)

Vrijmoed, J. C., Austrheim, H., John, T., Podladchikov, Y. Y.127. 2008. Metasomatism of the UHP Svartberget olivine-websterite body in the Western Gneiss Complex, Norway, Geophysical Re-search Abstracts, Vol. 10, EGU2008-A-09457. (Talk)

Vrijmoed, J. C., Podladchikov, Y. Y., Andersen, T.B.128. 2008. An alternative model for ultra-high pressure in the Svartberget oliv-ine-websterite, Western Gneiss Complex, Norway, Geophysical Research Abstracts, Vol. 10, EGU2008-A-08915 (Talk).

Webb, K.E.129. Pockmark ecology in fjords and offshore Norway. The 33rd International Geological Congress, Oslo (Talk).

Yarushina, V.M.130. Interdisciplinary Constraints on Solid Earth Dynamics from the Crust to the Core: An international Sym-posium in Honor of Prof. David Yuen’s 60th Birthday; Zurich, Switzerland. 3.06.-14.06. 2008. (Talk and Poster).

Yarushina, V.M. 131. Chimney-like porosity waves as a mechanism for fluid expulsion at low temperature environments. The Inter-national Conference on Mathematical Geophysics CMG2008, Longyearbyen on Spitsbergen, Norway. 15.06 – 18.06. 2008 (Talk and Poster)

Yarushina, V.M. 132. Microscale yielding as mechanism for low-fre-quency intrinsic seismic wave attenuation. 70

th EAGE Confer-

ence & Exhibition incorporating Spe Europec 2008, Rome, Italy. 12.06 -14.06. 2008 (Talk and Poster).

Yarushina V.M.133. Chimney-like porosity waves as a mechanism for fluid expulsios. Fourth Marie Curie Summer School ”Porous and Aqueous Materials” 19-29 August 2008, Trest, Czech Republic

Yarushina V.M., Podladchikov Y.Y.134. Low-frequency seismic wave attenuation in porous media due to microscale yielding. 33IGC, Oslo, 6 - 14 August, (Talk).

Yarushina V.M., Podladchikov Y.Y.135. Chimney-like porosity waves as a mechanism for fluid expulsion at low temperature environ-ments. 33IGC, Oslo, 6 - 14 August (Talk).

Yarushina, V.M., Podladchikov Y.Y.136. Chimney-like porosity waves as a mechanism for fluid expulsion. EGU, Vienna, Austria, April 13 – 19 2008 (Talk).

Yarushina, V.M., Podladchikov, Y.Y.137. Low-frequency seismic wave attenuation due to microplasticity in porous media. The Kongsberg seminar 7-9 May 2008 (Poster).

Ydersbond, Y., D.K. Dysthe.138. The dynamic brittle-ductile tran-sition in extrusion processes. The Kongsberg seminar 7-9 May 2008 (Poster).

Other talksAarnes, I.1. Naturkatastrofer med betydning for vår tid. Fredrikstad og omegns geologiske forening 3.11.08. Talk.

Jamtveit, B.2. Supervulkaner, Nesbru Rotary Club, Asker, 28 Jan 2008

Jamtveit, B. 3. Forskning og administrasjon: Om retning og fart på et tohodet troll. NUAS (Nordiske universitetsadministratorsamar-beidet) Conferece Blindern, Oslo, 13 June 2008.

Jamtveit, B.4. Om PGP’s aktivitet og samarbeid med institusjoner i Afrika, Asia, og Latin Amerika. Seminar for ”Nord-Sør utvalget” at UiO. 26 Aug 2008.

Svensen, H. 5. Årsakene til global oppvarming og masseutryddelser i jordens historie. Norsk geofysisk forenings symposium. Geilo, Norway, 18 Sept (Invited talk).


In the media 2008

RadioJamtveit, B.1. Commenting on the catastrophic 7.9M Earthquake in China on May 12th, Verdt å vite. NRK Radio P2. May 15, 2008.

Mazzini. A.2. Der Vulkan Lusi auf Java spuckt weiter Schlamm, Dradio-Deutschlandfunk, 7 May 2008 (interview).

Mazzini. A. 3. Radio interview on the BBC Radio 4 about “the Lusi mud disaster” 23 October 2008 (interview).

Svensen, H.4. Himalayas fjell. Verdt å vite 28.11.08 kl 12:05.

Svensen, H.5. De sub-glasiale Gamburtsevfjellene i Antarktis. Verdt å vite 4.12.08

Articles in magazines / booksGisler, G.1. Violent processes in Geophysics. Meta, 10-13.

Hammer, Ø.2. Livets historie. Geo no. 8 2008, p. 32-35.

Jamtveit, B.3. PGP: et fargerikt fellesskap - til glede for oljeindus-trien. Geo p.56-58 October 2008. (Interview)

Jamtveit, B.4. Jordens indre krefter. Geo p44-48, oktober 2008.

Jamtveit, B.5. Jordens indre krefter’, NRK, P2-akademiet, Bind XXXX, Transit, Oslo, p-114-125.

Mair, K.6. Stanser jordskjelv midt i utviklingen. Nytt fra eVita nr 2, 2008 (interview).

Mazzini, A.7. How to make a volcano. Geoscientist 18. June 2008 (interview).

Mazzini, A.8. An unnatural disaster in Indonesia, Geotimes, August 2008 (interview)

Mazzini, A.9. Indonesian mud volcano may not be man-made, New Scientist, January 2008 (interview)

Mazzini, A.10. A different kind of eruption wreaks havoc in East Java, National Geographic, January 2008 (interview).

Mazzini, A.11. Debate over Indonesian mud volcano reignites. The New Scientist, Volume 200, Issue 2681, 5 November 2008, Page 6.

Mazzini, A.12. Der unendliche Matsch. Süddeutsche Zeitung no 181, page 16, 2008 (interview).

Planke, S.13. Revealing the secrets of volcanic sedimentary basins. Geo June 2008, 16-22.

Ramberg I.B., Jansen E, Olesen O., 14. Torsvik, T.H. 2008. What does the future hold? Geohazards, climate change and continental drift. In Ramberg I., Bryhn I., Nøttvedt A. & Rangnes K. (eds.): The making of a land: Geology of Norway. The Norwegian Geological Association, 560-591.

Torsvik, T.H.15. & Steinberger, B. 2008. From continental drift to mantle dynamics. In ”Geology for Society for 150 Years - The lega-cy after Kjerulf”, eds. T. Slagstad & R. Dahl. Gråsteinen 12, 24-38.

NewspapersSvensen, H.1. Dommedag på alvor. Morgenbladet 17 October 2008 (Interview).

Lønstad, T. Workshop i ødemarka. (Interview with A. Nermoen 2. and participants of the PGP thermodynamics course). Oppland Arbeiderblad 3 November No. 256, page 3.

Online newspapers and magazines Braeck, S., Podladchikov, Y.Y., Medvedev, S.1. 2008. Spontaneous dissipation of elastic energy by self-localasing thermal runaway: http://arxiv.org/PS_cache/arxiv/pdf/0805/0805.3292v1.pdf

Løvholt, F., 2. Gisler, G. Overdreven frykt for LaPalma-tsunamien. Forskning. No 10.4.08 (Interview).

Mazzini. A.3. Kein Ende der Schlammschlacht, Deutschlandfunk, 7 May 2008 (interview in web article).

Mazzini, A.4. A Wound in The Earth, Time, 28 February 2008 (in-terview).

Mazzini, A.5. Indonesian mud volcano unleashes a torrent of con-troversy. News of the Week. 2 February p. 586 (interwiev).

Mazzini, A.6. Mud eruption ’caused by drilling’. BBC News 1 Nov 2008 (interwiev).

Mazzini, A.7. Geologists blame drilling for Indonesian mud volcano. Nwe Scientist 31 October 2008 (interwiev).

Mazzini, A.8. What caused the LUSI mud volcano eruption? Inno-vations report 14.10.2008 (interwiev).

Mazzini, A.9. Indonesian oil company blamed for mud disaster. En-erpub 1 November 2008 (interwiev).

Mazzini, A.10. Experts Clash Over Mud Disaster - Theories on Trig-ger of Indonesian Mud Volcano. PR Web 22 October (interwiev).

Mazzini, A.11. Two Years On, a Mud Volcano Still Rages--and Bewil-ders. News of the Week 13 June (interview).

Mazzini, A.12. Unstoppable. Science 13 June 2008 (interview).

Mazzini, A.13. Norwegian researcher studies Lapindo mudflow Indo-nesia News Blog 27 February (interview).

Mazzini, A.14. Mud volcano cause discussed. AAPG Expolrer, page 32-33.

Mazzini, A.15. AAPG Meeting Pins Mudflow On Drilling. Pesa News Resourses December 2008/January 2009 (interview).

Mazzini, A.16. Indonesian Mus Flow History. Satnews Daily ¨,De-cember 2008.

Mazzini, A.17. Indonesian oil company blamed for mud disaster. En-erPub 1 November.

Mazzini, A.18. Lapindo Brantas ”responsible” for mud flow. AsiaN-ews.it, 31 october (interview).

Mazzini, A.19. Experts Clash Over Mud Disaster - Theories on Trig-ger of Indonesian Mud Volcano. PR Web 22 October.

Mazzini, A.20. Vexing Mud Flow Cause Disputed. Explorer July 2008.

Morgan, J. 21. Mud eruption ”caused by drilling” BBC News. (Web article including interview with A. Mazzini).

Other activities Galland, O.,1. Sassier, C. Andean geotrail 2008-2009

Svensen, H.2. Stand-up researcher during Forskningsdagene at UiO. In Frokostkjelleren in the old ,central universityi sentrum, 25. sep-tember.


Appendices

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PGP University of Oslo

PO Box 1048 Blindern N-0316 Oslo

Norway

phone: (+47) 22 85 61 11fax: (+47) 22 85 51 01http://www.fys.uio.no/[email protected]

Annual Report 2008

PGP

COVERPHOTO: Satelite image of East Greenland, showing fjords stretching from the cost and ca. 400 km westwards to the Greenland icesheet. The fjordsystem locally cuts 4 km down from the old ‘paleosurface’ and is a classical example of a fractal landscape. In a 2008 Geology paper, Medvedev, Hartz and Podladchikov presented a geodynamic model that explains how erosion caused more than 1.2 km of uplift, thereby solving a century long enigma of why Mesozoic marine rocks form high mountains in Greenland. Sateliteimage by NASA (http://visibleearth.nasa.gov/)

Documents

PGP Achievements 2007 in brief PG… · his work on the book “Fjellenes historie” (the history of the mountains) in 2008. His 2006 book “Enden er nær” was pub-lished in English