Annual Report 2008 PGP

Transcription

Annual Report 2008
2008
Annual Report
PGP
PGP Achievements 2007 in brief
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 invitations we choose to accept. The number of contributed presentations at conferences was 136 (85 at international meetings 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 collaborators and students.
geological wintermeeting in January 2009; Marcin Krotkiewski 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 Norwegian Academy of Science and Letters in 2010-2011. Francois 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
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PGP products 2003-2008
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120
100
2003
2004
2005
2006
2007
2008
80
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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 researchers are working in academic institutions abroad.
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20
0
Papers in reviewed
journals
Papers in press
Papers in
books, proceedings
TV & Radio
Newspapers &
magazines
Invited talks
Conf. Presentations
4 Guest students visited PGP for one semester, and 15 invited
scientists gave talks at PGP in 2008.
400
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.
PGP ISI citations
350
300
250
200
Several PGP students received awards and recognitions in
2008. Luiza Angheluta received an ‘Outstanding student poster 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
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100
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2003
PGP Annual Report 2008
2004
2005
2006
2007
2008
Table of Contents
PGP Achievements 2008 in brief............................................ 2
Directors comments ................................................................. 4
Physics of Geological Processes .............................................. 5
Mission Statement ................................................................. 5
Main Challenges ...................................................................... 5
Aim ............................................................................................. 5
Scientific status – Main projects ............................................ 6
A. Geodynamics ........................................................................ 7
B. Fluid processes................................................................... 16
C. Localisation processes...................................................... 32
D. Microstructures.................................................................. 38
E. Interface processes ......................................................... 44
Education ................................................................................... 52
Petromax and Industry funded projects .............................. 54
Public relations ......................................................................... 55
Organisation ............................................................................ 56
Infrastructure and laboratories ............................................ 59
Finances ..................................................................................... 61
Appendices ............................................................................... 63
List of staff .......................................................................... 64
Student list ........................................................................... 66
Numerical models ................................................................. 68
Registered field work .......................................................... 69
Project portfolio .................................................................. 69
Invited talks 2008 ................................................................. 72
Experimental laboratory activities .................................... 72
Production list ....................................................................... 74
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Director’s comments
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), including 1 in Nature, 1 in Nature physics, 1 in Reviews in geophysics, 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 combination 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 satisfactory 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 international 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 postdoc Espen Jettestuen got a position as researcher at IRIS (the
International Research Institute of Stavanger). He will however, keep an adjunct researcher positon at PGP.
Among our students, Marcin Dabrowski continues as a postdoc and group coordinator at PGP after having received his
PhD in June. Evgeny Tanzerev finished in September and accepted 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 Eriksen works for the company Volcanic Basin and Petroleum Research. By the end of 2008, 26 students have graduated from
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PGP. 24 of these are in paid jobs. 9 are working in petroleum
companies or in companies doing petroleum-related business, 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 researcher Adriano Mazzini have been published in a wide range
of media including: radio interviews by BBC and DradioDeutschlandfunk, 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 published 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
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‘our’ artist Ellen Karin Mæhlum was displayed at the 33
International Geological Conference at Lillestrøm in August.
A new exhibit by Mæhlum, inspired by compaction experiments, 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 projects with visible relevance towards energy and environment.
This is reflected by our most recent major projects: Two EUprojects started, or was granted, in 2008. The EU Network
project ‘Delta-min’, includes Haakon Austrheim, Bjørn Jamtveit, and two new PhD students (Jörn Hövelmann and Oliver
Plümper). Our new postdoc, Julien Scheibert, received an EU
Physics of Geological Processes
Mission Statement
Our mission is to obtain
Marie Curie grant for his project ‘Earthcracks’ in collaboration 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 collaborative project on CO -sequestration between Haakon Aus2
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 fundamental geological processes. Our prime goals are to continue our cross-disciplinary crusade to provide quantitative
understanding of how the Earth works and to produce students with a unique competence to address problems of
relevance for both science and society.
• 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 Challenges
Our main challenges are
• establishing an adequate conceptual framework for
dealing with the Earth’s complex materials and processes
• attracting highly qualified national and international
scientists and students
Aim
Our 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 integrated 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
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Scientific status – Main projects
Introduction
From 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 emergence of spatial and temporal patterns, as cooperative phenomena. A comprehensive understanding of these phenomena 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.
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.
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.
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A. Geodynamics
1. Towards a global reference frame linking plate motions and
processes in the deep Earth interior
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 system 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 convection into account, and we have connected this to a pre–100
o
Ma global palaeomagnetic frame adjusted 5 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 rotation of the entire Earth relative to its spin axis: True Polar 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 characteristics of TPW (“stop-and-go” motions, in particular coherent 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).
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.
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A. Geodynamics
Using plate-driving force arguments and the mapping of reconstructed Large Igneous Provinces to Core–Mantle Boundary 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 understanding in fields as diverse as palaeogeography, palaeobiology, long-term environmental evolution, tectonics and Earth
history on the grandest scale.
References
Steinberger, B., Torsvik, T.H. 2008. Absolute plate motions 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, 273283.
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.
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A. Geodynamics
2. Stability of Boundary Layers in Turbulent Mantle Convection
Models
We investigated the stability of boundary layer anomalies
of the Earth’s mantle under conditions of vigorous convection. Geophysical studies have revealed the existence of pronounced 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 temperatures in cratonic keels. Archean cratons contain all of the
major diamond deposits on our planet. Dating of diamond inclusions from Archean kimberlite pipes yielded Archean ages
for the formation of the diamonds, meaning that Archean lithosphere 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 numerical mantle convection models.
We devised a new, dynamic thermal Finite Element Method
(FEM) mantle convection model and apply more realistic viscosity ratios between the cold, rigid lithosphere and the hot
sublithospheric mantle. Our assumptions about realistic viscosity ratios are based on extrapolation of results from laboratory 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 quantitative 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 relationship 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 whereas the sublithospheric mantle behaves like a viscous fluid. We
found no significant difference between viscous and viscoelastic models for the question of craton stability (Beuchert et al.,
2009).
Yet, stress fields inside the lithosphere differ significantly between viscous and viscoelastic rheologies (Figure A3). Thus, if
accurate stresses are to be predicted inside the lithosphere in
dynamic mantle convection simulations, a viscoelastic rheology 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
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 viscosities. 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 vigorous 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 between surrounding mantle and LLSVPs being a phase boundary 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 dynamically 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 partially 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 Africa 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 support our suggestion by an open channel flow approximation
in which dense LLSVPs material can flow towards the equator under the influence of centrifugal forces in relatively short
time given realistically low viscosities (Beuchert and Podladchikov, 2009a).
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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.
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A. Geodynamics
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.
References
Beuchert, M.J., Podladchikov, Y.Y. 2009a. Long-term stability 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.
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A. Geodynamics
3. Work on Caledonian high and ultra-high pressure rocks in western Norway
The joint work between T.B. Andersen (PGP) and Brad Hacker (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 established. 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 published 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, Vrijmoed 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).
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References
Andersen, T. B., Jamtveit, B., Dewey, J. F., Swensson,
E. 1991. Subduction and Eduction of ContinentalCrust - 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., KylanderClark, A., Peterman, E., Walsh, E., Young, D. Deformation during continental margin subduction and exhumation: 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, Western Gneiss Region of Norway. Journal of Metamorphic
Geology, 21, 613-629.
Johnston, S., Hacker, B. R., Andersen, T. B. 2007. Exhuming Norwegian ultrahigh-pressure rocks: Overprinting
extensional structures and the role of the NordfjordSogn 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: Implications 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 Svartberget 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).
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A. Geodynamics
4. Stress-drop determinations from subduction related palaeoearthquakes
in mantle rocks from Alpine Corsica
Results of PGP research on blueschist and eclogite facies
pseudotachylytes in the Alpine parts of Corsica has been published 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 decorated by thin films of ultramafic pseudotachylyte to constrain
the stress during seismic faulting that formed the pseudotahylyte. 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 uncontrovertably show that mantle lithosphere is able to sustain very
large stresses during subduction/collision. We have demonstrated that stress-drops of more than 5.8 kbar were released
by earthquakes at intermediate depth (≥1.5 GPa). These minimum stresses were obtained by calculating the minimum release of energy that goes into formation (heating + melting) of
pseudotachylytes along faults with known minimum displacements (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.
References
Andersen, 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. Pseudotachylytes from Corsica: fossil earthquakes from a subduction 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
The work on the Corsican pseudotachylytes has been carried
out as a collaboration between the geodynamic and localization group, and the results of the stress determinations have
already been used in new work by PGP researchers on mechanism of intermediate to deep earthquakes (John et al. 2009).
The work continues in 2009 with focus on the petrology of the
ultramafic pseudotachylytes.
14
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.
15
B. Fluid processes
Introduction
1. Venting and climate effects
The Fluid Processes group at PGP continues the activities
from previous years in partly overlapping subjects of venting and climate effects, fluidised systems, pockmarks, sill emplacement, 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 fragmentation; 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.
Central Scientific Problem
Gases 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 analysis 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 environmental 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 hydrothermal 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 hydrocarbon reservoirs.
Recent Results
The 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 (Svensen et al. 2009). The Siberian Traps Large Igneous Province
emplaced sill intrusions into a vast region (Figure B1) containing 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
16
ormerly Vendian). Furthermore, enormous volumes of Cambrian
aporites are present in the basin, with up to 2.5 km thick sequences
halite-rich strata, anhydrite, and carbonates (Fig. 2) (Zharkov, 1984;
trychenko et al., 2005). Five major phases of salt deposition occurred
the Cambrian, the most extensive being the 2 million km2 Early
mbrian Usolye salt basin with an average of 200 m of halite (Zharkov,
84). Note that the “Tunguska Basin” in the literature is frequently
cluded in the terms “Siberian Platform” and “Siberian Craton”, and that
e Tunguska Basin is often considered as one of many basins situated on
e platform/craton. We use the term to encompass all the post Neooterozoic sedimentary rocks on the platform/craton.
The total thickness of the basin stratigraphy commonly varies
tween 3 km and 12.5 km (Meyerhoff, 1980; Kontorovich et al., 1997),
wever the Neo-Proterozoic rocks are locally present as 7–10 km
ick rift segment deposits (Sokolov et al., 1992; Kuznetsov, 1997;
obot et al., 2004). Post-Cambrian rocks comprise carbonates, marls,
the stratigraphy (Meyerhoff, 1980; Fedorenko and Czamanske, 1997;
Ulmishek, 2001). The maximum accumulated sill thickness in the
Cambrian to Permian strata is 1200 m (Kontorovich et al., 1997). The
thickness of sill intrusions in the Neo-Proterozoic rocks is uncertain due
to 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 the
Cambrian evaporate sequence (Kontorovich et al., 1997; Ulmishek,
2001). The present day area with outcropping sill intrusions is at least
1.6 million km2 (Fig. 1). The sill emplacement led to widespread contact
metamorphism of the host sediments (e.g., Kontorovich et al., 1997) and
to enhanced maturation of organic matter and the formation of
methane-rich petroleum accumulations (Sokolov et al., 1992). The
most profound results of the magma-sediment interaction are spectacular magnetite-rich breccia pipes rooted in the Cambrian evaporites or
possibly deeper. These pipes are numerous in the southern parts of the
basin, where they are filled with up to 700 m deep and 1.6 km wide
B. Fluid processes
. 1. Geological map of the Tunguska Figure
Basin in Eastern
Siberia, Russia.
Note
abundance
of phreatomagmatic
pipes withRussia,
magnetite
south of latitude 64, and the numerous basaltB1 Geological
map
of the
thehigh
Tunguska
Basin
in Eastern Siberia,
showing
ed 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 is
the distribution of of phreatomagmatic pipes with magnetite in the south and with
dified from Malich 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 der
basalt in the north. Our main study area during a 2004 field campaign is indicated by
ass 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.
2
the star symbol. The Cambrian evaporite comprises a total area of 2 million km .
17
B. Fluid processes
from boreholes drilled decades previously for potash prospecting (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 layers, resulting in an outgassing much more rapid than occurred
in other Large Igneous Provinces.
H. Svensen et al. / Earth and Planetary Science Letters 277 (2009) 490–500
493
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 Cambrian
Figgure B2 Composite cross section from the Nepa locality (star in Figure B1). The location map shows four of
evaporite 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 presented
the Nepa
boreholes
we have
studied
inthedetail
three
pipes.
The (Verkholensk
CambrianSuite),
evaporite
strata are
here. The topmost
stratigraphic
unit isthat
Ordovician
(O), and
the rest of
drilled and
sequences
arebreccia
from the Late
Cambrian
Middle Cambrian
(Litvintsev Suite,
abbreviated
L-S), and the
Cambrian (Angara
Suite
and Bulay Suite,
abbreviated
B-S). The
sill is sometimes
referred to as the Usol'epipe
sill (Zamaraev
et al.,the
1985).
overlain
byLower
Ordovician
clastic
sediments.
Core
data from
theUpper
6G hole
in the Scholokhovskoie
and from
194 hole have been analysed.
4. Results
(e.g., Raymond and Murchison, 1989, 1991; Galushkin, 1997; Fjeldskaar
et al., 2008). This implies that the total volume of sediments affected by
4.1. The breccia
contact metamorphism is equal to twice the sill volume. Note that the
gas will be produced in the aureole independent of the specific type of
The magmatic fragments of the Scholokhovskoie pipe are rich in
organic material undergoing metamorphism (dispersed organic matter,
18
glass
(Fig. 4), demonstrating rapid melt quenching in the pipe, and the
coal beds, or petroleum). The mass conversion factors for
calculating
PGP
Annualgas
Report
2008
pipe formation was accordingly contemporaneous with the sill emequivalents from carbon are 1.34 and 3.66 for methane and carbon
B. Fluid processes
497
H. Svensen et al. / Earth and Planetary Science Letters 277 (2009) 490–500
Fig. 6. Schematic evolution
theSchematic
Tunguska Basin
pipes andof
thethe
venting
of carbon
gases and
halocarbons
the atmosphere.
The pipe
evolution
is partly based Von der Flaass and
Figure ofB3
evolution
Tunguska
Basin
pipes
and thetoventing
of carbon
gases
and halocarbons
Naumov (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,
to the atmosphere. (1) Emplacement of sills into organic-rich sediments and evaporites with petroleum
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)
accumulations (P). (2) Contact metamorphism of shale, evaporite, and petroleum, leading to gas generation
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.
(shown
as stippled
lines).inMelt
accumulates
within
evaporite
sequences4)in
the source
region
Powerful eruptions and
led tooverpressure
wide craters and
subsidence.
Gases generated
contact
aureoles are now
released
to the atmosphere.
Continued
degassing
from both magma and
(3)crater-lake.
Pipe formation
and eruption.
Glass organic-rich
in the breccias
shows
the
magma
was disrupted
and
sediments through of
thethe
pipepipe.
and the
Contact metamorphism
of shallow
sequences
(coal)that
along
dikes,
and appearance
of the first
lava flows further to the
fragmented
the source
regioninbefore
vertical
transport
and phreatomagmatism.
Powerful
led
wide
north in the basin. The
inferred gasincomposition
is shown
the frame,
alongside
the estimated
carbon gas and halocarbon
productioneruptions
potential for
theto
pipe
degassing alone.
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
sequences
(coal)
along dikes, and
theoffirst
flowsstratigraphy
further to the
north the
in precise nature
by our experiments.
Gasorganic-rich
generation from
sediment
metamorphism
is appearance
close to theofbase
thelava
evaporite
although
thethe
basin.
known both from
Karoo Basin in South Africa and offshore Norway,
of the roots remains unknown. Fig. 6 shows the schematic evolution of
resulting in vertical piercement structures (Jamtveit et al., 2004; Svensen
the pipe structures. The sizes of the pipe craters in the Tunguska Basin
et al., 2004; Svensen et al., 2007). The main differences in the pipe
suggest powerful eruptions, with gases and ash likely reaching high
forming mechanisms between these two settings and the one in Siberia,
atmospheric levels. The presence of glass in the Scholokhovskoie breccia
is the presence of evaporites and petroleum in the source region, and
pipe suggests that the pipe was formed as a phreatomagmatic event,
extensive magma-sediment interactions within the pipes. The pipes are
where the partly molten magma cooled rapidly in the pipe during
rooted at
2–4
km
depth
in
magma-sediment
mixing
zones,
probably
eruption. Parts of the wall-rock collapsed into the pipe, mixing with the
References
Svensen, 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-Sørenssen, A., Corfu, B., Jamtveit, B. 2007. Hydrothermal
venting of greenhouse gases triggering Early Jurassic
global warming. Earth and Planetary Science Letters,
256, 554-566.
Svensen, H., Planke, S., Polozov, A. G., Schmidbauer,
N. Corfu, F., Podladchikov, Y. Y., Jamtveit, B. 2009.
Siberian gas venting and the end-Permian environmental crisis. Earth and Planetary Science Letters, 277,
490-500.
19
B. Fluid processes
2. Fluidised and partly fluidised systems
Much 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 important 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 Results
Active eruptions of mud volcanoes provide excellent opportunities 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 environmental 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 eruptive 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 recent years, activity from the seeps has fluctuated, with methane and petroleum flares occurring occasionally (Figure B5).
The active seep locations are coincident with caldera collapse
20
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 conduct experiments in which fluids are injected into boxes containing 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 different sizes, in order to quantify the conditions of fluidisation
and segregation of particles. One such experiment is illustrated 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 concentration 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 neighbouring chimneys as they do.
Computer simulations are another way of studying fluidised
systems. Galen Gisler has used the multi-material hydrocode 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 becomes conical, rather than straight, and the surface eruption
(as in Figure B8) is like a geyser.
6
B. Fluid processes
ARTICLE IN PRESS
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.
A. Mazzini et al. / Marine and Petroleum Geology xxx (2008) 1–13
te image of the Dashgil mud volcano; (B) interpreted mud flows corresponding to previous eruptions. At least three possible eruption events can be dis
line in eruption II might represent the border between two separate events, however satellite and field observations are inconclusive to solve this amb
epresents the most recent eruption. Flows older than I cannot be excluded but cross correlations are hard to be established.
his article in press as: Mazzini, A., et al., When mud volcanoes sleep: Insight from seep geochemistry at the Dashgil mud
Marine and Petroleum Geology (2008), doi:10.1016/j.marpetgeo.2008.11.003
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.
21
B. Fluid processes
ARTICLE IN PRESS
A. Mazzini et al. / Marine and Petroleum Geology xxx (2008) 1–13
11
Fig. 7. (A) NW–SE section of Dashgil MV. Vertical axis not to scale. The marked locations in and aro
Figure B6 (A) NW–SE section of Dashgil MV. Vertical axis not to scale. The
locations
inmargin;
and around
crater
diffusemarked
seepage along
the outer fault
and (3) salsathe
lakes.
Symbols in the stratigraphy:
shales/sandstones;
M ¼the
Maikop-shales;
(B) magnification
of area
image A highlighting th
represent respectively: (1) The gryphon field inside the crater; (2) diffuse seepage
along
outer fault
margin;
andframed
(3) insalsa
13
seepage. Seepages outside the crater show stronger d CCO2 depletion and higher amount of CH4. A
lakes. (B) Magnification of area framed in image A highlighting the collapse
controlled
by
faults
that
act
as
preferential
interpreted plumbing system of gryphon-pool complex based on field observations and gas/wat
deep fluids migrate,
mixingfluids
with shallow
meteoric waters.
gryphon
pathways for the seepage of deeper fluids. At large salsa lakes deep fluidswhich
andtheshallow
meteoric
converge
and At
mix.
(C)sites evaporatio
morphologically (e.g. from pools) ‘‘isolating’’ the fluids inside the crater and in the internal chamb
Interpreted plumbing system of gryphon-pool complex based on field observations
and gas/water analyses. Overburden of the
allowing a bypass through the intervals charged with meteoric fluids.
gryphons causes collapse and fractures through which the deep fluids migrate, mixing with shallow meteoric waters.
moderate 13C depletion and higher amount of C2þ homologues are
commonly interpreted as thermogenic deep-rooted gas that rises
rapidly towards the surface (e.g. Blinova et al., 2003). See Etiope et al.
(in press, 2008b) for a more extensive explanation of the global
statistics of gas seeping from mud volcanoes worldwide.
Comparison between gas sampled from the Dashgil MV and
that from the neighboring oil fields (Katz et al., 2002) gives insight
about the mechanisms of gas migration. Katz et al. (2002) show that
numerous of the reservoir gases from the South Caspian were
not generated in situ and have been altered and/or represent mixed
B7
Fluidisation
experiment
a bimodal
isotopic
signatures of the gas
source
hydrocarbons.
The d13CCH4with
seep
2). Li
most
dept
from
field
gesti
et al.
to m
Table
pres
Figure
distribution of grain sizes. Air is injected at high speed into
Please cite this article in press as: Mazzini, A., et al., When mud volcanoes slee
the bottom
of a Hele-Shaw cell containing a large number of
Azerbaijan, Marine and Petroleum Geology (2008), doi:10.1016/j.marpetgeo.2
small grains and a smaller number of large grains. Because
a region
containing
more
grains than the average is
g. 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 large
crater; (2)
fuse seepage along the outer fault margin; and (3) salsa lakes. Symbols in the stratigraphy: PT ¼ Productive Serie-sandstones;
Sarmatian-shales;
TC ¼particles
Tarkan–ChokrakmoreS ¼permeable,
the
tend to segregate into chimneys
ales/sandstones; M ¼ Maikop-shales; (B) magnification of area framed in image A highlighting the collapse controlled by faults that act as preferential pathways for deeper fluids
mainly
large grains.
and shallow meteoric
fluids converge
and mix; (C)They coalesce into fewer,
epage. Seepages outside the crater show stronger d13CCO2 depletion and higher amount of CH4. At large salsa lakes deep fluidscontaining
terpreted plumbing system of gryphon-pool complex based on field observations and gas/water analyses. Overburden of the
gryphons
causes spread
collapse and
fractures through
more
widely
chimneys
as they grow towards the
hich 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 differ
surface.
18
orphologically (e.g. from pools) ‘‘isolating’’ the fluids inside the crater and in the internal chambers. d O values support a confined seepage of fluids through the feeder channel
owing a bypass through the intervals charged with meteoric fluids.
oderate 13C depletion and higher amount of C2þ homologues are
ommonly interpreted as thermogenic deep-rooted gas that rises
pidly towards the surface (e.g. Blinova et al., 2003). See Etiope et al.
n press, 2008b) for a more extensive explanation of the global
atistics of gas seeping from mud volcanoes worldwide.
Comparison between gas sampled from the Dashgil MV and
at from the neighboring oil fields (Katz et al., 2002) gives insight
bout the mechanisms of gas migration. Katz et al. (2002) show that
umerous of the reservoir gases from the South Caspian were
ot generated in situ and have been altered and/or represent mixed
ource hydrocarbons. The d13CCH4 isotopic signatures of the gas
seeping at Dashgil are similar to those from deeper oil field gas (Table
2). Like also pointed out by Katz et al. (2002), our results suggest that
most of the deeper-sited thermogenic mature (?) gas migrates from
depth greater than 3 km and that there is a negligible contribution
from shallow biogenic methane. However the d13CCH4 of Dashgil oil
field is slightly lower than the neighboring reservoirs (Table 2) suggesting a small biogenic input. Similarly to what pointed out by Etiope
et al. (in press) our data also suggests that isotopic fractionation related
to microbial oxidation is not significant. Yet the seeping gases (Fig. 5A,
Table 2) show dramatically lower amounts of the C2 component and
presence of C3þ only in some cases and anyhow in negligible amounts
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
22
B. Fluid processes
ARTICLE IN PRESS
G. Gisler / Marine and Petroleum Geology xxx (2009) 1–8
B8 Simulation
with
theportion
Sage code
eruption
high pressure
fluids through
a 11.5
deformable
medium,
representing
g. 6. Log Figgure
density raster
images from the
central
of the of
runthe
shown
in Fig. 5of
(Smu07),
shown at intervals
of 1 s, from
s through 16.5
s. The violence
of the breakout rips
a sedimentary
basin.toThis
image and
shows
a sequence
intervals of 1 second, in a calculation in which a pipe is formed by the
aterial from
the surface adjacent
the opening
entrains
it into the at
flow.
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
ngle of approximately 45� towards the surface. These cracks often
propagating vertical cracks and upward-propagating diagonal
medium’s strength is insufficient to hold them open against the dynamic pressure of the released volatiles.
ave a side-to-side asymmetry, with one crack propagating further
cracks form throughout the block. The configuration after 50 s is
r faster than the other. The asymmetry is initiated by round-off
shown in the appropriate block in Fig. 3.
rror and grows because of stress concentration at the crack tip.
References
own-propagating cracks start at the surface in these simulations:
3.2.Mazzini
Run SmuO7:
straight-sided
pipe Processes
with outburst
A. 2009.
Mud Volcanism:
and ImplicaBahr, A., Pape, T., Bohrmann, G., Mazzini, A., Haeckel,
he surface bows upwards as the diagonal cracks grow, increasing
tions (Editor). Marine and Petroleum Geology Journal,
M., Reitz, A., Ivanov, M. 2008. Authigenic carbonate
he tensile stress near the centre until failure occurs.
ASpecial
nearly straight-sided
Issue (in press).vertical pipe is formed in the SmuO7 run,
precipitates
from
the NE
Black Sea:
a mineralogical,
At higher pressures
and
higher
velocities
(to the
right and down
illustrated
in
Fig.
5, with H.,
an injection
pressure
of 0.8 kbar
Mazzini,
A.,
Svensen,
Akhmanov,
G.G., Aloisi,
G., and speed
geochemical
and
lipid
biomarker
study.
International
n Table 1 and Fig. 3), the diagonal cracks are suppressed: they often
of 500
m/s. That
is, we keep the A.,
same
injection
speed
Planke,
S.,
Malthe-Sørenssen,
Istadi,
B.
2007.
Trig- as in the
Journal
of
Earth
Sciences,
DOI.
10.1007/s00531-007orm and then anneal. The behaviour is instead dominated by the
previous
run,
but
increase
the injection
pressure.
gering
and
dynamic
evolution
of
the
LUSI
mud
vol0264-1.
ormation of a vertical pipe to the surface, tending towards conical
Once
the calculation
starts off Science
with the
ram and static
cano,again,
Indonesia.
Earth and Planetary
Letters,
Cronin,(higher
B., Çelik,
H., Hurst,
Gul, M., but
Gürbüz,
K., at
t higher energies
pressures
or A.,
velocities),
straighter
pressure
of the injected fluid producing considerable compaction
261,
375-388.
Mazzini,
A.,
Overstolz,
M.
2008.
Slope-channel
Comower energies. The pipe is sometimes accompanied by horizontal
and
therefore
ahead
the working surface.
Mazzini,
A. jamming
Nermoen,immediately
M. Krotkiewski,
Y. of
Podladchikov,
plex
Fill and
Overbank
Tinkernot
Channel,
pening-mode
cracks
leading
off inArchitecture,
either direction,
always
Initial
crack
propagation
therefore
starts
sideways.
A compaction
H. Svensen, S. Planke, 2009. Fault shearing as a mechKirkgecit Formation, Turkey. In: T.H. Nilsen, R.D.
ymmetrically.
wave
propagates
away
from
the
injection
point
at
anism for overpressure release and trigger for pierce-the acoustic
Shew, G.S. Steffens and J.R.J. Studlick (Editors), Atlas
speed
in the
sediments
(5 km/s).for
The
wave returns to
ment
structures.
Implications
therarefaction
Lusi mud volcano,
of Deep-Water Outcrops. AAPG Studies in Geology, 56,
the
injection
point
in
just
under
1
s,
reducing
the
jamming just
1. Run SmtO7:
cone sheets?
Indonesia. Marine and petroleum Geology (accepted)
363-367.
enough that the ram pressure can force the opening of a vertical
Mazzini, A., Svensen, H., Planke, S., Guliyev, I., AkhGisler, G. 2009. Simulations of the explosive eruption of
crack. By 4 s (Fig. 5, top frame), this crack has come to within 1.2 km
As an example
of diagonal
development
propagation,
manov, G.G., Fallik, T., Banks, D. 2009. When mud
superheated
fluidscrack
through
deformableand
media.
Marine
of the surface, and its walls have compacted and hardened to
we chose to and
focusPetroleum
on the very
nearly
symmetrical
configuration
volcanoes sleep: Insight from seep geochemistry at the
Geology
Journal,
Special Issue.
a density of 1.3 g/cc.
eveloped Ivanov,
by run M.,
SmtO7,
which
has an E.,
injection
pressure
of
Dashgil mud volcano, Azerbaijan. Marine and PetroBlinova,
V., Kozlova,
Westbrook,
G.,
At 10 s (Fig. 5, middle frame), a number of diagonal cracks have
.6 kbar and an
injection
of 500
Three
snapshots
leum Geology, doi:10.1016/j.marpetgeo.2008.11.003.
Mazzini,
A.,speed
Minshull,
T. m/s.
Nouzé,
H. density
2007. First
samspawned off the gaping vertical crack, whose tip is now within
om this run pling
are shown
in Fig. 4.from the Vøring Plateau. EOS, 88,
Skinner Jr, J.A., Mazzini, A. 2009. Martian mud volcaof gas hydrate
275 m of the surface. Some downward-propagating cracks have
Just 1 s after
the start of the calculation (Fig. 4, top), a small
nism: Terrestrial analogies and implications for forma209-210.
started from the surface to meet the big crack. By 25 s (Fig. 5,
avity has opened
upA.,
above
theM.K.,
top ofNermoen,
the rigid A.,
injection
pipe.
The
tional scenarios. Marine and Petroleum Geology (in
Mazzini,
Ivanov,
Bahr, A.,
Borhbottom frame), the crack has relaxed to a narrower width, with
ediments immediately
above this
are
crushed
a density
of 1.3 g/
press).
mann, G., Svensen,
H.,
Planke,
S. to
2008.
Complex
fluid streaming vigorously upwards and exploding outwards
c, nearly halfplumbing
solid density,
byinthe
and ram pressure
of the
Svensen, H., Hammer, Ø., Mazzini, A., Onderdonk,
systems
thestatic
near subsurface:
geometries
of
through the funnel-like crater. A significant amount of fragmented
uid exiting the
pipe (see
inset at top
right).
Further propagation
in
N., Polteau, S., Planke, S., Podladchikov, Y. Y. 2009.
authigenic
carbonates
from
Dolgovskoy
Mound (Black
sedimentary material is entrained in the flow, both as large chunks
he vertical direction
is blocked
by jamming,
and the Marine
fluid seeks
Dynamics of hydrothermal seeps from the Salton Sea
Sea) constrained
by analogue
experiments.
&
and fines.
asier paths to
the side. Geology, 25, 457-472.
geothermal system (California, USA) constrained by
Petroleum
In an animation of this simulation, the vent is seen to open
After 10 s (middle frame), the diagonal cracks have progressed
temperature monitoring and time series analysis. Jourviolently at about 12 s, with significant erosion and entrainment of
bout a quarter of the way to the surface, more compaction above
nal of Geophysical Research (in review).
material from near the opening. This is illustrated in Fig. 6, in
he pipe has increased the sediment density to 1.6 g/cc. The added
a sequence of six frames from the animation, showing just the
olume below causes some bowing of the surface 1.7 km above,
breakout region, from 11.5 s to 15.5 s.
23
nitiating a downward-propagating crack almost directly above
the
PGP Annual
Report 2008
njection pipe.
4
B. Fluid processes
3. Sill emplacement
Magmatic intrusions in sedimentary basins often form horizontal sills and frequently exhibit saucer-shaped morphologies. They are of significant economic interest because they affect oil maturation and migration pathways, form traps for petroleum 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.
Recent Results
Magmatic sill intrusions tend to develop saucer-like geometries 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 adjacent and nested saucers. Previous models for the emplacement of such saucer-shaped sills have usually been based on
analysis of the intrusion geometry and the spatial relationships
POLTEAU ET AL.: HOW ARE SAUCER-SHAPED SILLS EMPLACED?
B12104
with potential feeders, rather than on magma flow patterns.
Stephane Polteau (Polteau et al 2008) and
co-workers, using detailed field observations
and magnetic susceptibility measurements,
were able to infer flow
directions, and thereby
place constraints on the
emplacement mechanism. The data support
a model consisting of a
point feeder supplying
magma in a radial pattern to form the saucershaped sill, rather than
feeding by dikes.
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.
Figure 1. (a) Aerial view of the Golden Valley Sill. (b) Geological map of the Golden Valley Sill
Complex 24
showing the location of sampling sites (in general, one point corresponds to both opposite sill
Annual Report
2008
margins). X and Y axes are longitude and latitudePGP
in degrees.
(c) Simplified
geological cross section of
B. Fluid processes
A
Sediment dikes
Sediments
Dolerite sill
R67
B
C
Sediment
dike
Dolerite sill
Dolerite sill
Dolerite sill
Sediment dikes
E
D
Meta-sandstone
Dolerite
Dolerite
Sediment
dike
Dolerite
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.2(E) Close-up of a sediment dike showing sediment
Figure
fragments and the dolerite “bridge” extending from the walls and into the dike. Hammer for scale.
25
B. Fluid 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 contracting 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 surrounding medium and in some cases produce vent complexes directly leaking these volatiles into the atmosphere (Figure B11).
References
Aarnes, 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: Constraints 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 compressional settings: insights from geological examples
and experimental modelling, Bollettino Della Società
Geologica Italiana (In press).
Polteau, S., Mazzini, A., Galland, O., Planke, S., MaltheSørenssen, A. 2008. Saucer-shaped intrusions: Occurrences, emplacement and implications. Earth and
Polteau, S., 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. 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.).
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.
26
B. Fluid processes
4. Fluids and Sediments: Travertines and Pockmarks
The precipitation of suspended sediment from fluids in motion,
and the ablation and suspension of sediments removed from
topographic irregularities, shape patterns that occur worldwide in earth’s crust, including travertine terraces surrounding 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 Results
Travertine terracing is one of the most eye-catching phenomena in limestone caves and around hydrothermal springs, but
remains fairly poorly understood. The interactions between
water chemistry, precipitation kinetics, topography, hydrodynamics, carbon dioxide degassing, biology, erosion and sedimentation 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 precipitation localization at rims, a single explanation is probably
insufficient. Instead, a multitude of effects are likely to contribute, 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 pockmarks 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 groundwater, 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.
Figure B12. Shallow seismic
reflection studies of the Oslofjord
pockmarks.
27
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.
28
B. Fluid processes
Figure B14. Cross-section of a three-dimensional simulation of undersea currents
deflected by a seafloor pockmark.
References
Akhmetzhanov, 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 continental 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 instability 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 Publications (Accepted).
Hammer, Ø., Webb, K.E., Depreiter, D. Upwelling currents 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. Pockmarks 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).
29
B. Fluid processes
5. Violent processes
Many 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 fraction 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 compelling moral interest in understanding these events with the
ultimate goal of protecting and saving human lives.
Recent Results
The multi-material adaptive-mesh hydrocode Sage (from Los
Alamos and Science Applications International) has been applied to an increasing variety of violent processes in geophysics, including asteroid impacts, mud volcanism, and landslidedriven tsunamis.
In 2008, Galen Gisler made further studies of asteroid impact
models, examining the distribution of ejecta from oblique impacts 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 distributions, although butterfly patterns persist up to 60-degree
inclinations. Appreciable amounts of material can be moved
great distances without suffering high pressures or temperatures 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 localised, but large quantities of water tend to spread out the effects, making the damage less intense locally but more widespread. 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.
30
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 Canaries. 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 currents; too viscous, and the slide stops too early. High numerical resolution is important for treating this problem, so this
work continues. The implications of this study will have bearing 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).
References
Gisler, 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, Trondheim. (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.
31
C. Localisation processes
Introduction
1. Pore-scale inelasticity and seismic
Our research on the dynamics of deformation localisation
in the earth encompasses the brittle, transitional and ductile
deformation regimes, concentrating on meso-scale phenomena. 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 operating 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; Nonhydrostatic compaction and decompaction; and Hierarchical
fracturing during serpentinisation.
Scientific problem
In 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 attenuation 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 concluded that such a nonlinear mechanism was not relevant for
seismic waves. Recent observations, however, show the presence 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 seismic 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 microscopic stresses around cavities and inclusions may be much
higher than the macroscopic stress level.
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.
32
wave attentuation in reservoirs
Figure C2 Model of a representative volume
element of porous media.
Approach and results
We 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 porosity 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 evaluate 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, attenuation can be high and independent of both frequency and strain
amplitude.
References
Yarushina 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 seismic wave attenuation”, Conference proceedings, 70th
EAGE Conference & Exhibition — Rome, Italy, 9 - 12
June.
Figure C3 Model predictions and data collapse for
quality factor Q
33
2. Fragmentation and strain partitioning in faults
Scientific problem
Strain localization has important implications for the mechanical strength and stability of evolving fault zones. Structural
fabrics interpreted as strain localization textures are common in natural and laboratory faults, however, the dynamic
microscale processes controlling localization (and delocalization) are difficult to observe directly. Discrete numerical models 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.
We present a method that implements realistic gouge evolution 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-disperse spherical aggregate grains gradually evolves, with accumulated 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.
34
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.
References
Andersen, T.B., Mair, K., Austrheim, H., Podladchikov,
Y.Y., Vrijmoed, J.C. 2008. Stress-release in exhumed
intermediate-deep earthquakes determined from ultramafic pseudotachylyte. Geology, 36, 995-998.
Bjørk, T.E., Mair, K., and Austrheim H. 2009. Quantifying fault rocks and deformation: advantages of combining 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 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.
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.
35
3. Ultra-high pressure rocks
Scientific problem
Ultra-high pressure (UHP) rocks, recording mantle-like pressures (3.0 - 5.5 GPa) but hosted by mid-crustal (much lower
pressure) rocks are difficult to explain, particularly in continental collision orogens where no evidence for deep burial
(to UHP conditions) or extreme exhumation (from UHP conditions) exists. At Svartberget (W. Norway), a peridotite enclave 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) observed. In addition it is difficult to explain: i) Deformation of
the rheologically strong peridotitic rocks (forming brittle fractures 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.
References
Vrijmoed, J.C., Smith, D.C., van Roermund, H.L.M. 2008.
Raman confirmation of microdiamond in the Svartberget 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 Svartberget Fe-Ti garnet-peridotite, Western Gneiss Region,
Norway. European Journal of Mineralogy, (in press).
Vrijmoed, J.C. Pressure variations during ultra-high pressure metamorphism from single grain to outcrop scale?
Journal of Metamorphic Geology (soon to be submitted).
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 submitted)..
We have conducted an interdisciplinary study including detailed field mapping, petrography, mineral-chemistry, whole
rock (isotope) geochemistry, dating and numerical modelling 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 Ultra 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 brittle 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 overpressure. 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 rheologically strong rock, such as peridotite, could give rise to differential stresses that may explain the conjugate set of fractures
observed in the Svartberget peridotite.
36
(a)
(b)
felsic migmatitic gneiss
(b)
1m
(c)
P (GPa)
12
10
8
6
-
4
2
0
2.5
5
10 m
0
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.
37
D. Microstructures
Introduction
Introduction
The main focus of the microstructures group in 2008 has been
the study of the deformation of heterogeneous and/or anisotropic materials, the coupling to reactions, and the development 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 unstructured (body fitted) finite element method (FEM) code that is
capable of solving problems with more than 100’000’000 degrees 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” entitled “Recent Advances in Computational Geodynamics:
Theory, Numerics and Applications” and BILAMIN clearly
stands out in terms of state of the art computing in earth sciences. The second paper on folding is by Jäger et al. (2008)
entitled “Brittle fracture during folding of rocks: A finite element 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 technically challenging problem. The third paper on the deformation 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 information 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.
38
After some trouble with publishing our concept of “mechanical closure” we finally succeeded and two papers now document 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 previous 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 research 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 Jettestuen. 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 orientation) anisotropy. Nevertheless, mechanical material anisotropy is usually ignored in structural geological and tectonic
models, often due to theoretical or numerical complications.
Marcin Dabrowski has studied the role of mechanical anisotropy 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 effective anisotropic material properties of deforming heterogeneous materials.
D. Microstructures
1. Stokesian Dynamics
Overview
The 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 approach is to give up on the body fitting mesh requirement and
to use regular grids. Introducing operator splitting the complexity 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 developed 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 parameter. 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 particles (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 assumption of underlying analytical solutions becomes invalid.
2) Since the individual particle problem has to be solvable
analytically the particle geometries have to be simple, preferentially 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 suspensions, 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 solution for large numbers of particles (>10’000) difficult because
of memory and CPU requirements.
The advantages of the Stokesian dynamics approach are obvious by looking at the characteristics of the corresponding PGP
code: StokesDyn. StokesDyn runs on a standard desktop computer and can solve systems with thousands of particles up to
large strains within a day. The involved particles are truly rigid, 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 complements 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, especially three dimensional ones such as produced by StokesDyn. 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.
39
D. Microstructures
Figure D1 Visualization of a Stokesian dynamics result.
Figure D1 shows the result of a Stokesian dynamics calculation that is visualized with the free rendering engine POVRay (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 unstable 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
40
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. However, it seems that because we are trained to perceive scientific
results in abstract illustrations the photorealistic result visualization almost gives a “non-scientific” impression. However,
photorealistic result rendering can be used in a complementary fashion in scientific visualization.
D. Microstructures
2. Mechanical Anisotropy Development of a Two-Phase
Composite Subject to Large Deformation
Anisotropic
DEM
Anisotropic
DEM
Anisotropic
DEM Anisotropic DEM
Anisotropic DEM
In
theDEM,
two
dimensional
anisotropic
DEM,
the
medium
is man
con
Anisotropic
Inthe
the
two
dimensional
anisotropic
DEM,
the
medium
is constructed
in iterative
an
iterative
InIn
the
twotwo
dimensional
anisotropic
theDEM,
medium
is constructed
in conan
manner
The overallAnisotropic
mechanical
response of a heterogeneous rock
may DEM
dimensional
anisotropic
the
medium
is
DEM
In the two dimensional anisotropic DEM, the medium is constructed in an ite
Anisotropic
DEM
become
anisotropic
due
to
the
development
of
shape
preferred
structed
in
an
iterative
manner
by
placing
a
given
area
fraction
ofofaligned
individual
given
area
fraction
fiterative
In the
two dimensional
anisotropic
DEM,
is constructed
in an
manner
by
b in
ofa aligned
individual
inclusions
of
aspect
ratio
placing
a given
area
fraction
a b ainclus
off aligned
individual
inclusions
aspect
ratio
into
placing
a given
area
fraction
f medium
In the two dimensional anisotropic DEM, the medium
is constructed
in an
iterative
manner
bytheplacing
of aligned
individual
inclusions
of aspect r
a given inclusions
area fraction off aspect
f of aligned
a b into
(SPO).
Laminated
materials
a maximal
deindividual
ratio
the
In theorientation
two dimensional
anisotropic
DEM, the
medium exhibit
is constructed
in
an iterative
manner
by placing
a
b
of
aligned
individual
inclusions
of
aspect
ratio
into
the
placing
a
given
area
fraction
hostproperties
and reevaluating
theiteration
hoststep.
properties
after
eachand
iteration
st
reevaluating
the
step.
Both,
inclusion
and
and and
reevaluating
properties
afterafter
eacheach
iteration
Both,
inclusion
hosthost
ph
af b the
of host
aspect
ratio
intohost
thehost
placing a given area fraction f of aligned individual inclusionshost
gree of anisotropy, where shear and normal viscosities assume a bhost and reevaluating
the host
properties
eachiteration
iteration
host and reevaluating
the host
propertiesafter
afterincleach
step. Both, inclusi
incl
ratio
into the
the host
placing a given area fraction f of aligned individual inclusions of aspect
incl
host
host
host
and
reevaluating
properties
after
each
iteration
step.
Both,
inclusion
and
host
phase
R norm
 
arehost
isotropic
and
the
viscosity
ratio
is normal
. The
areinclusion
isotropic
and
the
inclusion
host
viscosity
ratio
. The
effective
Ris R  host
and
arestep.
isotropic
and
thehost
inclusion
host
viscosity
ratio
isinclusion
effective
host and reevaluating
host properties
iteration
step. Both,
and
phase
values corresponding
to thethe
lower
(Reuss) after
and each
upper
(Voigt)
Both,
inclusion
and
phase
are
isotropic
the
inare isotropic and the inclusion host
viscosity
ratio is R   incl  host
incl
host
eff . The effe
host and
reevaluating
the host properties
after
each
iteration
step.
Both,are
inclusion
host
phase
eff
incl and
host
eff
R




.
The
effective
normal
isotropic
and
the
inclusion
host
viscosity
ratio
is
theoretical
bounds.
However,
the
model
of
a
laminate
is
not
clusion
host
viscosity
ratio
is
.
The
effective
norn
and
shear
viscosities
are two
obtained
by ordinary
integrating
tw
by
 and. and
 n are
are isotropic and the inclusion host viscosity ratio is R  
The
effective
normal
shear
viscosities
are
obtained
by
integrating
coupled
diffe
shear
viscosities
obtained
integrating
two
coupled
ordinary
differen
 seff  seff
s
incl
eff
suitable
the viscosity
transient
stage
the
anisotropy
evo- normal
and
areobtained
obtained
integrating

 host . The effective
are isotropic
andfor
thestudying
inclusion host
ratio
is Rof
andshear
shear  seff viscosities
viscosities are
bybyintegrating
two coupled ord
eff mal  n
and shear
viscosities
are differential
obtained by
integrating two coupled ordinary differential
equations
s
equations
and the
shear
viscosities
are as
obtained
by in
integrating
two coupled
ordinary
 seffbuild
equations
lution during
SPO
up, such
depicted
Figure D3.
two
coupled
ordinary differential equations
equations
and shear  seff viscosities are obtained by integrating two coupled
ordinary
differential
equations
A major improvement
is the anisotropic self consistent
averequations
 eff  
d  nd  n 1 1
 eff effdn  1 eff R   
equations
  n 1
aging (SCA) model developed by Fletcher (2004) that incor
   RdR
n
n
eff



eff df
1 f
n
 R n 
df df 1  1f  efff  
  eff RR
n
1
R  
d  n of finite
 eff   and is free of dany
1
porates the effects
SPO magnitude

 R   n  eff df 1  f  n n n  eff R  n  
(
 eff  R   n 
eff
df
1  f d  d  1 1R  n    eff  ds  1
d n

1
 eff  
1 f parameters.
phenomenological
scheme is not
 eff RThe
 n SCA

s

s
 R   ndf fitting
R



(1)
s 
 s(1)
   R  R
 eff    s   eff   R 
df
f composites
1 for
eff
 eff R with
  distinct inclusion-host
optimal
geometry
df df 1  1f efffds  1eff R
s Rs 1s  f
d s
1
Rdf
s
d s
 eff  
1 n
(1)
eff
R





df
1 f
s
  R s
 effand
  s  viscosity ratios. For example,
 Rlarge
atd high
concentrations
df
1 f
1
 eff eff R host
df
1 f  
s
s
eff
eff
 eff   R  s
eff eff effeff eff eff

effwhere
eff
host
 R  to
2eff
values
 values
a bof
b
,initial
andinitial
host
s  interchanging




,
, n,and
where








s. The
where
,
,




itdfis insensitive
the
weak
and
strong
phase
at
where
s
 aeff,b a bb ab/ an2. /The
 
sand
n hostn ns, s  eff
1 f
 n,s   n,s   n,s   n,s 
eff
 eff   R  s
eff






a
b  b a  / 2 . The ini
,
,
and
where





eff
eff n , s  eff
eff
host
n
s
n
,
s


50% concentration.
For
circular
inclusions,
the
SCA
prediction
 n of
b  b a  / 2 . The initial values of  n
where  n, sa / 
, values
and  are
 initial
 a 1.
, sThe
2The
where  n, s   effn, s   host ,  eff  neff  eff
values
.nand
and
ofs n ,and
 s 1.
are 1.
s , and    a b  b
s are 1.
 s initial
and
are
eff mean
eff
eff the inclusion and host viscosieff
host
a
geometrical
of







a
b

b
a
/
2
,
,
and
.
The
initial
values
of
whereisjust






and
are
1.
n
n
s
s
 n,s 
 n,s 
and  s the
are 1.
and  s of
arewhether
1.
ties irrespective
a strong or weak phase forms
and load-bearing
s are 1.
host. Thus, the effective viscosity is not bounded
Using finite element modeling allows us to directly resolve
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 effective 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.
the anisotropic mechanical response of composites consisting
of aligned inclusions. We systematically scan through the parameter 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.
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.
41
D. Microstructures
The DEM approach does not only provide estimates 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 calculated 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 cannot be captured with the DEM approach. The underlying analytical solution is for elliptical inclusions 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 developed DEM scheme is applicable to cases such as
shown in Figure 3b.
a)
b)
Figure D4 shows how the shear viscosity evolves
Comparison between the DEM prediction and the FEM result obtained for the Error! Reference source not
in the FEM model depicted in Figure D3 as a funcfound.b configuration.
Error! Reference
found.
how theitshear
viscosity
evolves in the FEM model
tion of source
shear not
strain
andshows
compares
to the
DEM
Strain rate intensity
The source
DEM not
scheme
depicted inprediction.
Error! Reference
found. performs
as a functionsurprisof shear strain and compares it to
ingly well and no significant deviations between
FEM and DEM are discernable up to large strains.
between FEM and DEM are discernable up to large strains. The DEM accurately predicts an
The DEM accurately predicts an initial increase
initial increase
in effective
the effective
shearviscosity
viscosity  xyeff (up
(up to
then a pronounced drop
in the
shear
to   1 ) )and
and
then
a
pronounced
drop
under
the
initial
value.
The
increase
under the initial value. The increase is an effect of the development of the mechanical
is an effect of the development of the mechanical anisotropy
anisotropy due to the emerging SPO, the drop is related to the reorientation of the anisotropy.
due to the emerging SPO, the drop is related to the reorientaThis microstructural
weakening
may provide
viable explanation of
the strain weakening
tion of the
anisotropy.
This amicrostructural
weakening
may that is
often observed
in deforming
materials.
in the analyzed
linear
provide
a viable poly-phase
explanation
of theHowever,
strain weakening
that
is viscous
often
observed
in
deforming
poly-phase
materials.
However,
cases the degree of weakening is not sufficient to result in a strong localization on spatial scales
in the analyzed linear viscous cases the degree of weakening
larger than the inclusion size and other effects such as non-linear rheology (power law), lattice
is not sufficient to result in a strong localization on spatial
preferred orientation, or dynamic recrystallization resulting in a grain size reduction should be
scales larger than the inclusion size and other effects such as
considerednon-linear
in addition. rheology (power law), lattice preferred orientation,
or dynamic recrystallization resulting in a grain size reduction
should be considered in addition.
the DEM prediction. The DEM scheme performs surprisingly well and no significant deviations
0
0.2
42
0.4
0.6
0.8
1
1.2
1.4
1.6
1.8
2
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
Conclusions
1
0.9
0.8
Effective viscosity
The developed anisotropic DEM model provides a better estimate over SCA for higher concentrations of inclusions. The
discrepancies between the scheme predictions reflect a fundamental 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 viable explanation of a strain weakening observed in poly-phase
materials. The model is applicable to any deformation path
and constrains constitutive laws incorporating structural evolution factors that are employed in large scale, geodynamic
simulations.
Voigt bound
0.7
0.6
0.5
0.4
0.3
FEM
0.2
References
Austrheim, H., Putnis, C.V., Engvik, A.K., Putnis,
A., 2008. Zircon coronas around Fe-Ti oxides: a physical 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. Unpublished 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.
DEM
0.1
Reuss bound
0
0.5
1
1.5
2
2.5
3
Simple shear magnitude
Figure D4 Comparison between the DEM
prediction and the FEM result obtained for the
Figure 3b configuration.
Milke, R. et al. 2009. Matrix rheology effects on reaction
rim growth I: evidence from orthopyroxene rim growth
experiments. Journal of Metamorphic Geology, 27, 7182.
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 Metamorphic 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.
43
E. Interface processes group
Mechano-chemical transformation processes
Scientific problem
A 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 macroscopic relevance as the rate limiting factor for reaction progress.
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 mechanical 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 coupling 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 permeabilities, or reactions associated with major changes in porosities
or solid volume.
We have therefore developed models that address the mechano-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 access 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.
44
Recently, we developed a numerical and theoretical framework
to address the front dynamics in fracturing-accelerated reaction front dynamics. We have applied and tested the modeling
framework to study diffusion-controlled volume changing reactions, 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 general 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 eclogitization, or to an increase in volume for expansion processes
such as many weathering reactions.
We have applied this modeling approach to address the volume-increasing processes occuring during sphereoidal weathering. We have demonstrated how local volume-increasing
reactions may produce a large-scale hierarchical fracture pattern, and how this hierarchical process has a first-order impact 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 hierarchical 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 serpentinization 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 modeling to address the replacement of leucite by analcime, which
is a common process in silica-poor igneous rocks, and typically results in a 10% volume increase. The fracture pattern
observed on micron scale using back-scattered electron images closely resemble the hierarchical fracture structure seen
in comparable simulations (See Figure E3.)
a
b
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.
c
0
log10()
-0.5
-1
-1.5
Theory (acc)
Theory (noacc)
Simulation (acc)
Simulation (noacc)
-2
Simulation images
-0.2
0
0.2
0.4
0.6
log10(t/t0)
0.8
1
1.2
1.4
c
t
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.
45
Scientific outlook
We 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 predictions of the models against data from real systems. In particular, 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 interatomic bonding. Over the next year, we expect to be able to
bind the experimental and theoretical activities close together,
(a)
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.
References
Jamtveit, 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 processes. Contributions to Mineral Petrology, 157, 127133.
Røyne, A., Jamtveit, B., Mathiesen, J., Malthe-Sørenssen, A. 2008. Controls on weathering rates by reaction
induced hierarchical fracturing. Earth and Planetary
Science Letters, 275, 364-369.
(b)
(c)
46
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.
The thermodynamics and roughening of solid-solid interfaces
Scientific problem
At every turn in nature we are confronted with complex patterns. Patterns often formed in multiphase systems by an intricate dynamics of mass transport, e.g. diffusion and/or advection, 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 particular, have been discussed intensively such as the ATG instability at the surface of stressed solids in contact with their melt
or solution.
In the absence of surface tension, the instability manifests itself 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 dynamics 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 important 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 associated with isochemical transformations.
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 ρρlower=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.
When two solids are compressed transverse to an interface
separating them, we have shown that, if a phase transformation is possible, it can lead to a morphological instability, as
well as the development of fingers along the propagating interface (see Figure E4).
We have performed a stability analysis based on the Gibbs
potential for non-hydrostatically stressed solids and have established a linear relationship between the rate of entropy
production at the interface and the rate of mass exchange between 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.
47
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 densityρρ2. 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).
We have demonstrated that the morphological stability provide important information about the type of phase transformation process occurring at the interface of contacting solids
and readily provide information about the material parameters.
Scientific outlook
The interplay between the microscopic and macroscopic
physics is a fundamental problem in research on complex systems. 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 anisotropy on solid-solid phase transformations and the slow evolution of faults.
48
While most faults evolve with a characteristic stick-slip behavior, 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 underlying 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.
References
Angheluta, L., Jettestuen, E., Mathiesen, J. 2009. The
thermodynamics and roughening of solid-solid interfaces. 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 shrinkage-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 generate 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 substrate. 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. During 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 typically 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 prevailing gradient in material contraction whereas spirals are
formed in the presence of a radial gradient in the contraction
of a thin elastic layer.
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.
References
Cohen, Y., Mathiesen, J., Procaccia,I. 2009. Drying patterns: Sensitivity to residual stresses., arXiv:0901.0797.
49
An experimental study of stylolite formation
M.sc. thesis by Ola Kaas Eriksen
Stylolites are features of localized dissolution in sedimentary
rocks. They are planes oriented normal to the compaction direction and have a rough and often teeth-like surface structure. 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 diffusion 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 develops 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 diffusion length. A modeling study that explains the mechanisms of
these ductile compaction bands is underway.
Figure E8: Vertical autocorrelation of the final volume matrix
in Figure 1.
Figure E7: Deformation map of compacted granular material
showing ductile compaction bands. Color scale is the local
volume relative to original volume.
50
Extrusion of plastic crystals
Energy dissipation in a simulated fault system
M.sc. thesis by Yngve Ydersbond
Yngve Ydersbond has performed experiments on extrusion
processes. This is important in both industry and geological
settings. The transition from ductile 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 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 crystalline 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 velocity 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.
M.sc. thesis by Munib Sarwar
Movement 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 dissipated in an earthquake is in plate tectonic physics partitioned
into three different components Wtot = Wseismic +Wexpansion +Wfricwhere Wtot is the total work. The only part of the energy
tion
budget of earthquakes that can be measured directly is Wseismic,
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.
51
Education
Bachelor
The 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.
Master
Physics
PGP-physics
Material science
Geology
PGP master program
The 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.
PGP-geology
Geophysics
Mathematics
PGP-simulation
Computer science
For 2008, the master program has the following construction:
4 semester
Specialization courses
Master thesis
Master thesis
3 semester
Master thesis
Master thesis
2 semester
Master thesis
Master thesis
1 semester
FYS-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
The master project provides a practical introduction to scientific 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 – Disordered systems and percolation.
52
Geology: GEO4230 – Basin formation and sequence stratigraphy, GEO4250 – Reservoir geology, GEO4260 – Reservoir geophysics, yGEO4620 – Seismic waves and seismology,
GEO4630 - Geodynamics, Analytical methods in geochemistry, GEO4840 - Tectonics, GEO4850 – Advanced structural
geology.
Applied mathematics: MEK4550 – The finite element method
in solid mechanics I, INF-MAT5370 - Trianguleringer og anvendelser, INF5600 - Iterative methods and multigrid, INF5620
- Numerical methods for partial differential equations
Teaching and examinations
The PGP master program was externally evaluated in 2008.
The committee recommended to extend the scientific communication 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 students. 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.
Three Masters in PGP graduated and 2 PGP students defended 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).
Teaching statistics from FS by 10 March 2009:
Fys-Geo courses
Course title
Responsible
Given
Fys-Geo4110Scientific comm.
Fys-Geo4200/9200Case study
Fys-Geo4300Methods
Fys-Geo4510Mechanical geomod
Fys-Geo4520Thermodyn.geomod
Gisler
Austrheim
Dysthe
Podladchikov
Podladchikov
Autumn 08
Autumn 08
Autumn 08
Spring 08
Autumn 08
# reg.
students
7
2/1
4
5/7
2/2
Average
grade
Passed
B
B
Passed
Passed
Other courses
Course title
Geo4830
Geo4840
Gel2130
Geo4810
Fys-Mek1110
Fys-Mef1110
Fys2150
Fys4190
Fys4460
Bio4210
Bio4230
Bio4240
Responsible /involved
H. Austrheim
T.B.Andersen
D.W.Schmid /T.B. Andersen, M. Adamuszek
A. Beinlich
A. Malthe-Sørensen
A. Malthe-Sørensen
D.K. Dysthe
A. Mathiesen
A. Malthe-Sørensen
/Ø. Hammer, 5 hours
Comment
Autumn
Spring
Autumn
Autumn
Spring, 140 students
Spring
Spring
Spring
Spring, 5 students
Autumn
Spring
Spring
53
Petromax & industry funded projects
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
nd
of the 22 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 StatoilHydro which is involved in both the phase transition and
PetroBar projects. New development of the TECTMOD2D
software has been undertaken in collaboration with Geomodeling Solutions. PGP was further awarded a Ph.D. project
from VISTA on shear heating in 2008. The project will commence in 2009.
A major PGP activity is related to formation, migration and climatic impact of hydrocarbon fluids and gases. A large project
on mechanisms of primary migration was funded by PETROMAKS 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 volcano 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 greenhouse gases from metamorphic aureoles around sill intrusions. 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 MidNorway and the Karoo Basin in South Africa. Our new data
and theoretical models show that great quantities of hydrocarbon gases were generated just after the emplacement of the
o
more than 1000 C hot magma. The release of these gases in
hydrothermal vent complexes may have caused major environmental 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 cooperation between the Norwegian Academy of Science and Letters and StatoilHydro.
Table 1. Industry-related externally funded projects at PGP in 2008.
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
54
Public relations
PGP is becoming established as a leading institution in promoting science to the general public. We have an active relationship 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 researchers 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:
• PGP’s own popular science writing continues, and articles by Øyvind Hammer, Sverre Planke, Bjørn Jamtveit,
and Galen Gisler have been published in magazines
like GEO and Meta.
• The Andean Geotrail Project, where PGP researcher
Olivier Galland cycles along the Andes Mountains,
started in late fall 2008 and continues in 2009. Updates
are available on the web.
• Continued coverage of PGP results on the LUSI mud
volcano, headed by Adriano Mazzini. Interviews with
Mazzini have been published in media like Geotimes,
New Scientist, National Geographic, Süddeutsche Zeitung, Time, and Science.
(From Science, 13 June 2008)
55
Organization
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, administration and technical and financial delivery. The director reports to the board.
PGP board
Åm (head)
Aharony
Blundy
Bouchaud
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 coordinators for media contact, industry contact, field activities
and education. The coordinators, the administrative manager
and the director have regular meetings.
Financial and administrative organization
at PGP (by December 2008)
Putnis
Gabrielsen
Myhre
PGP director
Jamtveit
Administration
Research coord.:
-Admin. manager: Knudsen
-Admin. secretary: Brastad
-Lab support: Gundersen
-IT support: Christopher
-Industry: Planke
-Education: Andersen
-Media: Svensen
-Field: John
PGP core projects:
56
Geodynamics
Fluid
Processes
A
B
MicroInterface
Localistructures Processes
zation
Processes
C
D
E
Coordinator
Coordinator
Coordinator
Coordinator
Coordinator
Postdocs
Ph.Dstudents
MS-students
Postdocs
Ph.Dstudents
MS-students
Postdocs
Ph.Dstudents
MS-students
Postdocs
Ph.Dstudents
MS-students
Postdocs
Ph.Dstudents
MS-students
NRC
YFF
Petrobar
IPY
International
funding
EU
MIT
Industry &
Other
research
institutions
NGU
Aker Expl.
UiO
“Start
Packages”
PhD
positions
Permanent
positions
PGP Scientific organization 2008
A
B
PGP Director
Bjørn Jamtveit
C
D
E
Geodynamics
Fluid Processes
Localization
Micro structures
Interface
Coordinator:
S. Medvedev
Coordinator:
G. Gisler
Coordinator:
K. Mair
Coordinator:
D. Schmid
Coordinator:
A. Malthe-Sørenssen
Postdocs:
T. John
N. Simon
Postdocs:
A. Mazzinii (HS)
S. Polteu (HS)
O. Galland (HS)
Postdocs:
S. Santucci (KM)
Postdocs:
E. Jettestuen (BJ)
M. Dabrowski (DS,
from July)
Postdocs:
Christophe Raufaste
(AMS)
PhD students:
M. Beuchert (YPP)
S. Tanzerev (YPP)
to October
C. Galerne (ERN,
to October)
J. Semprich (NS/JIF)
H. Vrijmoed (HA)
PhD students:
F. Nicolaisen (AMS)
I. Aarnes (HS)
K. Webb (ØH)
Kirsten Fristad (HS)
PhD students:
V. Yarushina (YPP)
T. Bjørk (KM)
Master students:
S. Munib (KM)
PhD students:
M. Krotkiewski (DS)
Master students:
Y.W. Ydersbond (DD)
PhD students:
S. DeVilliers (JF)
A.Røyne (DKD)
L. Angheluta (JM)
A. Nermoen (DD)
Master students:
O.K. Eriksen (DKD)
B. Oust (JM)
Master students:
Master students:
Magnus Løberg (YPP)
Staff
As for December 31 2008, 45 employees from 14 countries 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 addition, PGP has a techical-administrative staff of 3.9 manlabour 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.
PGP work force in 2008:
Title
Professors, seniors
and researchers
Professor emeriti
Postdoc
researchers
PhD students
Techn/admin. staff
at PGP
TOTAL:
Guest students
In addition to this, numerous short term visitors stayed
at PGP, of whom 15 gave invited talks at the PGP external seminar serie (see appendix).
Number
25
Man-l. years
Comment
17.3
1 came, 1 left
7
5.1
One added in
2008
2 came, 3 left
17w
13.5
5
3.9
57
4
39.8
3
Some not fully
funded in 2008. 5
came, 2 left after
PhD defence.
Including 1 tech.
at Dept. of Geosci.
Each staying for
at least 4 months
57
The board
PGP has a new board for its second five-year period. Its mandate is to ensure that the inventions and plans underlying the
contracts between the parties are fulfilled and completed within the adopted time frame. The board evaluates and advises on
the centre’s scientific performance and assesses recent progress and future strategies. The board shall further ensure that
the interaction between PGP and the host institution functions smoothly. The board reports to the MN-faculty.
The board consists of seven members. The chairman is a highlevel manager in a major petroleum company, while four board
members are scientists, two from physics and two from geosciences. 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 combined 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.
PGP employees 2003-2008
20,0
2003
18,0
2004
Man-labour years
16,0
14,0
2005
12,0
2006
10,0
2007
8,0
2008
6,0
4,0
2,0
0,0
Professors and researchers
Postdoctoral fellows
Doctoral students
Other personnel
The board members:
Name
Institution
Knut Åm (chairman)
Industry representative
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
58
Research area
Country
Norway
Infrastructure and laboratories
Computer and network support
PGP has invested in a simple 5 TByte server solution for backing up data stored on local computers. Because the amount of
data produced and obtained increases faster than the available 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 enables users to backup their data and have them available in
the laboratories, in their offices or from anywhere with a secure 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 instruments
The 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 (Caliber from Veeco) to extend our surface imaging capability.
With our scanning equipment we are now able to scan most
scales and surfaces.
Equipment
XY-range
Z-range
XY-resolution
Z-resolution
AFM
>90 micro m
>12micro 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
50micro m - 5 mm
25micro 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 experiments 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 experiments.
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.
59
Experimental facilities
PGP 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 ventilation 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 general 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/scratching 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.
Figure 2.
Scanning with the
interferometer, the
art is shown in the
background.
60
Finances
PGP had a total income of 42 479 thousand Norwegian kroner (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 postions 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-
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 constituted 61 % and 15 % of the costs, respectively, and operating
costs and investments constituted the remaining 24 %.
Accounting 2008
Type of financing
UiO
NRC
NRC
Project number
Income
UiO/MN grant
UiO permanent positions
SFF from NRC
International funding (EU, MIT)
Other NRC grants
Other/private grants
Basis
PGP
SFF
International
funding
Other
projects
ChevTex,
StatoilHydro,
Aker Expl
Accoring
to the
long-term
contract
with NRC
4 974
4 974
9 274
14 036
92
14 036
92
14 036
600
5 323
1 503
7 590
624
7 590
92
Transfer between accounts
-2 000
2 000
1 735
2 671
1 000
14 036
2 931
11 800
SUM income incl. transfer
GRAND
TOTAL
EU, MIT
SUM income
Transfer 2007-2008
Other
private
grants
5 323
9 093
7 283
1 000
2 531
1 000
34 518
33 724
0
7 961
12 731
17 771
10 261
92
1 624
42 479
Temporary positions
4 136
10 575
3 334
934
18 979
SUM temp. pos+overhead
4 271
11 796
4 195
1 077
21 339
23 639
UiO permanent positions
5 323
5 323
35
503
100
638
1 820
Costs
Overhead (-inn/+out)
Investments
Operating costs
135
1 221
861
143
2 360
427
3 157
3 869
92
413
7 958
8 596
10 085
SUM 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
0
SUM operating costs & inv.
462
3 660
3 969
All numbers are in 1000 NOK (kkr)
92
413
8 265
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.
61
PGP is on track financially also in 2008. The center had
794 kkr higher income than anticipated in the long term funding plan of the contract with the Norwegian Research Council. The financiation from other NRC projects was substantially 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 anticipated 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-supervicor for a PhD student at University of Oslo, payed by a
YFF grant to Susanne Buiter at NGU (The Norwegian Geological 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
NRC
YFF to Buiter,
NGU
Interntat.
funding
from EU
Coordinator:
A. Putnis,
Münster
EU:
DELTA-MIN
T.B.Andersen
(2008-2011)
PhD student:
K. Ghazian
H. Austrheim
(2008-2011)
ca. 3 700 kkr
2 PhD
students
from 2009
Internat.
funding
MIT:
Siberian
Traps
H. Svensen
(2008-2011)
TOT :US$ 93330
62
Other
private
grants
NGU
T. Torsvik
(2008-2010)
2100 kkr
Researcher:
S. Medvedev
UiO
financiation
Start package
Tiltak 150102
D.K. Dysthe
2008-2011
TOT: 863 kkr
(incl. 25%
Granted
from PGP)
2 new PhD
positions
(2008-2011)
D. Schmid:
M. Krotkiewski
(PGP-CMA)
Austrheim:
A. Beinlich
(PGP-DG)
TOT: 3846kkr
Appendices
Appendices
2008 List of staff .............................................................64
2008 Student list .............................................................66
2008 Numerical models ............................................... 68
2008 Fieldwork .............................................................. 69
2008 Project portfolio .................................................. 70
2008 Invited talks ......................................................... 72
2008 Experimental laboratory activities................... 72
2008 Production list ..................................................... 74
63
List of staff
Name
Title
% pos.
Permanent postions, financed directly from UiO
Project
From
To
Man-labour
year
Background
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
0,2
Norway/
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
0,2
Germany
Knudsen, Trine-Lise
Adm.
100
142042
17.06.2007
1,0
Norway
64
31.12.2008
Appendices
Mair Karen
Senior
100
142042
01.01.2005
31.12.2012
0,4
Great Britain
Mathiesen Joakim
Ass. Professor
100
142042
01.02.2009
Meakin, Paul
Professor II
29
142042
01.01.2008
NA
1,0
Denmark
31.12.2008
0,3
USA
Planke Sverre
Senior
Raufaste, Christophe
Postdoc
Renard Francois
Professor
Santucci, Stephane
Senior
Souche, Alban
vit.ass
Svensen Henrik
Tanzerev Evgenyi
Torsvik, Trond Helge
Professor
Vrijmoed Hans
20
142042
01.02.2003
31.01.2013
0,2
Norway
100
142042
01.01.2008
31.12.2009
1,0
France
20
142042
01.04.2003
31.03.2011
0,2
France
100
142042
01.01.2008
31.12.2008
1,0
France
100
142042
01.10.2008
31.12.2008
0,3
France
Senior
100
142042
01.09.2005
31.12.2012
1,0
Norway
PhD student
100
142042
11.12.2007
31.01.2008
0,1
Russia
20
142042
01.04.2007
31.03.2010
0,2
Norway
PhD student
100
142042
26.09.2008
31.12.2008
0,3
The
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
John Timm
Postdoc
100
142561
01.09.2008
31.10.2008
0,2
Germany
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
John Timm
Postdoc
100
142953
01.07.2008
30.08.2008
0,2
Germany
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
Other
12,8
5,9
65
Student list
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
5
Bjørk, Torbjørn
Mair Faults and fault rocks
UiO; with Dept.
of Geosci.
CoE, NRC
6
Beuchert, Marcus
Podladchikov
Crust-mantle interaction
NRC
7
De Villiers, Simon
Feder
Crumpled sheets
NRC
8
Dabrowski, Marcin*
June 08
NRC
9
Fristad, Kirsten
Svensen
Anisotropy and geterogeneity in finite deformation resolving vs. Upscaling
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
Numerical simulations of hydrothermal vent
NRC
14
Røyne, Anja
MaltheSørensen
Weathering
UiO; MN-fac
15
Semprich, Julia
Podladchikov
Basin formation
16
Souche, Alban
Andersen
The thermal evolution in sedimentary basins
NRC (Petromaks
at Dept. of
Geosci)
Vista
17
Tanserev, Evgeniy**
Podladchikov
18
Vrijmoed, Johannes
Podladchikov
19
Webb, Karen
Hammer
Time-reverse methods in modelling of diffusive, convective
and reactive transport
Fracturing, metamorphism and metasmonatism at ultrahigh pressure
Marine biogeology
NRC
20
Yarushina, Victorya
Podladchikov
Computational geophysics
NRC
NRC
NRC
UiO, MN-fac
* 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
66
Appendices
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
67
Numerical models
Particular characteristics of geological processes such as complex and strongly varying material properties in space and
time, development of strong localization, large strain, multiphysics and multi-scale requirements render commercial software packages not applicable or make their application as
much or more tedious than the development from scratch.
Table 1 (Incomplete) list of numerical models developed at PGP
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
68
Appendices
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 – 04.08
b) Marcus Buchert, Leaders: Peltonen, Holtta & Slabunov
2a) Sweden-NorwayIGC33 Post-Conference Excursion
34, Tectonostratigraphic transect through the Caledonides.
(including partly leadership).
b) J.C.Vrijmoed
3a) FysGeo 4300, Oslo area, 04.09.2008
b) T.B. Andersen, Andrea Latini, Marta Adamuszek, Kristin 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, 25.09-29.09.2008
b) 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 - August
b) Ebbe H. Hartz, Niels Hovius (University lecturer at Cambridge University) and their sons Torjus and Miro.
c) Book on childrens meeting with the Arctic
8a) Salton Sea, California, 8 - 13.12
b)Adriano Mazzini, Stephan Polteau, Anders Nermoen,
Kirsten Fristad
c) Work on hydrothermal venting
69
Project portfolio 2008
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:
Research school, Podladchikov (104020)
Funding, kkr:
UIO FINANCIATION:
Permanent positions (salary costs only)
Funding, kkr:
TOTAL UIO FINANCIATION:
SFF grant
Funding, kkr:
2 000
789
4 974
5 323
10 297
YFF grant Forvard and inverse Yuri Podladchikov,
162741/V00
PI: Yuri Podladchikov, UiO project 121114
Funding, kkr:
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
PI: J.I. Faleide DG/Yuri Podladchikov, UiO basis, tiltak
104026
Funding, kkr:
1 503
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:
Comment: Sluttrapport 30.9.09, projekt til
avslutning 31.3.2010
TOTAL FINANCIATION, OTHER NRC PROJECTS :
70
113
14 036
Petromax Petrobar, 175973/S30
Other NRC projects
1 652
7 590
Appendices
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:
Comment: Transferred 92 kkr from 2008. * in $
TOT. FINANCIATION, INTERNAT. GRANTS:
92
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:
Comment: Transferred 86 kkr from 2008. Terminates
31.12.09.
TOT. FINANCIATION, PRIVATE GRANTS :
300
1 000
71
Invited talks 2008
Experimental laboratory activities
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 solution 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 heterogeneities inferred from microearthquake observations at the
San Andreas Fault Observatory at Depth (SAFOD).
March 27: David Smith Paris, France. Selected topics on applying 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 controls displacement-length scaling of geologic structures?
February 28: Frederique Rolandone France. The evolution of
the brittle ductile transition during the earthquake cycle: constraints from the time-dependent depth distributions of aftershocks.
February 14: Steffen Abe RWTH Aachen University, Germany.
DEM simulations of normal faulting in a cohesive material.
January 31: Karel Schulmann Strasbourg, France. Vertical extrusion and horizontal channel flow: key mechanisms of exhumation in large hot. orogens
The number of experimental users and of experimental activities is increaseing The following gives an overview of the activities, 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 Gundersen knows all the experimental equipment and facilities and is
of considerable help in the development of new experimental
projects and setups.
1. Stéphane Santucci
Friction/fracture processes
This project is a part of the fault and fracturing project. It focuses 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 system
Part 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 motion. Thermal imaging of the frictional surface during scratching 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 single crystals
The 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 reactions. One experimental approach consists of looking at reaction fronts in a hydrating salt. Another approach focuses on
subcritical cracking in calcite.
4. Christophe Raufaste
Volume changes in solids induced by chemical alteration
The project deals with the coupling between mechanics and
chemical alteration. Different “model” materials are investigated to understand the effect of volume changes induced locally by chemical reaction. Experiments are performed under
optical microscope and the interface of reaction is imaged
down to a resolution of a few microns.
January 17: Ritske Huismans, Bergen. Complex Rifted Margins
Explained by Dynamical Models of Depth-Dependent Lithospheric Extension.
72
Appendices
5. Olivier Galland
Mechanisms of shallow magma emplacement
The experimental setup allows a coupled monitoring of magma pressure, deformation of model surface, and the 3D shape
of resulting intrusion. Such a dataset allows a precise quantification 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 pores
In order to study the fluid induced deformation we have performed four experiments during 2008:
6.1. Shearing as an effective triggering mechanism for the formation 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 reacts 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 affected by the interstitial fluid flow, through the so-called seepage 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 fracturing 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, supervisors: Dag Kristian Dysthe, François Renard, Knut Bjørlykke, Jens Jahren)
Calcite pressure solution: single-contact experiments
Processes 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 observation of the contact is done through reflected light, this make
possible to look at the contact and the Newton rings generated by it. Following the Newton rings displacement enables
the determination of the rate of calcite dissolution as a function of the applied stress.
8. Matthieu Angeli
Salt hydration with temperature Imbibition of porous media
Salt crystallization during drying of porous media
Salt crystallization is a very damaging process for the porous
sedimentary stones. This process is partly responsible for erosion 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 Kristian Dysthe)
An experimental study on the growth of stylolites
The aim of this project was to simulate experimentally the
growing of stylolites. The main part of this work was compacting 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 dynamics
Experiments on extrusion processes. The transition from ductile 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 conditions 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 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.
11. Dysthe with Nermoen, Yderbond, Kaas and Munib
The ‘PGP science museum’, a series of demonstration experiments.
73
2008 Production list
Publications in international journals 2008
1. Aarnes, 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.
2. Alvey, A., Gaina, C., Kusznir, N.J., Torsvik, T.H. 2008. Integrated
Crustal Thickness Mapping & Plate Reconstructions for the High
Arctic. Earth and Planetary Sciences, 274, 310-321.
3. Andersen, T.B., Mair, K., Austrheim, H.O., Podladchikov, Y.Y.,
Vrijmoed, J.C. 2008. Stress-release in exhumed intermediate-deep
earthquakes determined from ultramafic pseudotachylyte. Geology, 36, 995-998. 17. Glodny, J., Kûhn, A., Austrheim, H. 2008. Diffusion versus recrystallization processes in Rb-Sr geochronology: Isotopic relicts in
eclogite facies rocks, Western Gneiss Region, Norway. Geochimica
et Cosmochimica Acta, 72, 506-525.
18.Hammer, Ø. 2008. Pattern formation: Watch your step. Nature
Physics, 4, 265-266.
19.Hammer, Ø ., Dysthe, D.K ., Lelu, B., Lund, H., Meakin, P., Jamtveit, B . 2008. Calcite precipitaiton instability under laminar, openchannel flow. Geochim. Cosmochim. Acta, 72, 5009-5021.
20.Hartz, E.H., Podladchikov, Y.Y. 2008. Toasting the jelly sandwich:
The effect of shear heating on lithospheric geotherms and strength.
Geology, 36, 331–334.
4. 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.
21.Heine, C., Muller, R.D., Steinberger, B., Torsvik, T.H. 2008. Subsidence in intracontinental basins due to dynamic topography. Physics of the Earth and Planetary Interiors, 171, 252-264.
5. Austrheim, H., Prestvik, T. 2008. Rodingitization and hydration of
the oceanic lithosphere as developed in the Leka ophiolite, north
central Norway. Lithos, 104, 177-198.
22.Hopp, J., Trieloff, M., Brey, G.P., Woodland, A.B., Simon, N.S.C.,
Wijbrans, J.R., Siebel, W., Reitter, E. 2008. 40Ar/39Ar-ages of
phlogopite in mantle xenolites from South African kimberlites: Evidence for metasomatic mantle impregnation during the Kibaran
orogenic cycle. Lithos, 106, 351-364.
6. Austrheim, H., Putnis, C.V., Engvik, A.K., Putnis, A. 2008. Zircon
coronas around Fe-Ti oxides: a physical reference frame for metamorphic and metasomatic reactions. Contributions to Mineralogy
and Petrology, 156, 517-527.
7. Burke, K., Steinberger, B., Torsvik, T.H., Smethurst, M.A., 2008.
Plume Generation Zones at the margins of Large Low Shear Velocity Provinces on the Core-Mantle Boundary. Earth and Planetary
Sciences, 265, 49-60.
8. Dabrowski, M., Krotkiewski, M., Schmid, D.W. 2008. MILAMIN:
MATLAB-based FEM solver for large problems. Geochemistry,
Geophysics, and Geosystems, 9, Q04030.
9. Engvik, A.K., Andersen T.B., Wachmann, M. 2008. Inhomogeneous 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.
10.Engvik, A.K., Putnis, A., Fritz Gerald, J.D., Austrheim, H. 2008.
Albitization of granitic rocks: The mechanism of replacement of
oligoclase by albite. The Canandian Mineralogist 46,1401-1415.
11.Ferrando, S., Frezzotti, M.L., Neumann, E.-R., De Astis, Peccerillo,
A., Dereje, A., Gezahegn, Y., Teklevold, A. 2008. Composition and
geothermal structure of the lithosphere beneath the Ethiopian Plateau: evidence from mantle xenoliths in basanites, Injibara, Lake
Tana Province. Mineralogy and Petrology, 93, 47-78.
12.Galerne, C.Y., Neumann, E.R., Planke, S. 2008. Emplacement
Mechanisms of Sill Complexes: Information from the Geochemical Architecture of the Golden Valley Sill Complex, South Africa.
Journal of Volcanology and Geothermal Research, 177, 425-440.
13.Ganerød, M., Smethurst, M.A., Rousse, S., Torsvik, T.H., Prestvik, 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.
14.Galland, O., 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.
15.Gisler, G.R. 2008. Tsunami Simulations. Annual Review of Fluid
Mechanics, 40, 71-90.
16.Glodny, J., Kûhn, A., Austrheim, H. 2008. Geochronology of fluidinduced eclogite and amphibolite facies metamorphic reactions in
a subduction–collision system, Bergen Arcs, Norway. Contributions to Mineralogy and Petrology, 156, 27-48.
74
23.Iyer, K., Jamtveit, B., Mathiesen, J., Malthe-Sørenssen, A. Feder,
J. 2007. Reaction-assisted hierarchical fracturing during serpentinization. Earth and Planetary Science Letters, 267, 503-516.
24.Iyer, K., Austrheim, H., John, T. Jamtveit, B. 2008. Serpentinization of the oceanic lithosphere and some geochemical consequences: Constraints from the Leka Ophiolite Complex, Norway.
Chemical Geology, 249, 66-90.
25.Jamtveit, B., Malthe-Sørenssen, A. Kostenko, O. 2008. Reaction
enhanced permeability during retrogressive metamorphism. Earth
and Planetary Science Letters, 267, 620-627. 26.Jensen, M.H., Sneppen, K., Angheluta, L. Kolmogorov scaling
from random force fields. Europhysics Letters, 84, 10011.
27.Jeger 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.
28.John, T., Klemd, R., Gao, J., Garbe-Schönberg, C.-D. 2008. Traceelement 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.
29.Kaus B.J.P., Gerya T.V., Schmid D.W. 2008. Recent advances in
Computational Geodynamics: Theory, Numerics and Applications.
Physics of the Earth and Planetary Interiors. Vol. 171. 2-6.
30.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.
31.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.
32.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.
33.Mathiesen, J., Jensen, M.H., Bakke, J.Ø.H. 2008. Dimensions, Maximal Growth Sites and Optimization in the Dielectric Breakdown
Model. Phys. Review E77, 066203.
34.Mathiesen, J., Procaccia, I., Regev, I. 2008. Elasticity with arbitrarily shaped inhomogeneity. Physical Review E 77, 026606. PGP Annual Report 2008
Appendices
35.Mazzini, A., 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 Dolgovskoy Mound (Black Sea) constrained by analogue experiments.
Marine & Petroleum Geology, 25, 457-472.
36.Medvedev, S., Hartz, E.H., Podladchikov, Y.Y. 2008. Vertical
motions of the fjord regions of central East Greenland: Impact of
glacial erosion, deposition, and isostasy. Geology, 36, 539–542.
37.Montes-Hernandez, Fernandez-Martinez, A., Charlet, L., Renard,
0
F., Scheinost, A., Bueno, M. 2008. Synthesis of a Se calcite composite using hydrothermal carbonation of Ca(OH)_2 coupled to a
complex selenocystine fragmentation. Crystal Growth & Design,
8, 2497-2504.
38.Montes-Hernandez, Fernandez-Martinez, A., Charlet, L., Tisserand, D., Renard, F. 2008. Textural properties of synthetic nanocalcite produced by hydrothermal carbonation of calcium hydroxide. Journal of Crystal Growth, 310, 2946-2953.
39.Perez-Lopez, R., Montes-Hernandez, G., Nieto, J.M., Renard,
F., Charlet, L. 2008. Carbonation of alkaline paper mill waste to
reduce CO greenhouse gas emissions into the atmosphere. Ap2
plied Geochemistry, 23, 2292-2300.
40.Pollok, K., Lloyd, G.E., Austrheim, H., Putnis, H. 2008. Complex
replacement patterns in garnets from Bergen arc eclogites: A combined EBSD and analytical TEM study. Chemie der Erde Geochemistry, 68, 177-191.
41.Polteau S., 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.
42.Polteau, S., Mazzini, A., Galland, O., Planke, S., Malthe-Sørenssen, A. 2008. Saucer-shaped intrusions: occurrences, emplacement
and implications. Earth and Planetary Science Letters, 266, 195204. 43.Rey, S.S,. Planke, S., Symonds, P.A. 2009. Seismic volcano stratigraphy of the Gascoyne Margin, Western Australia. Journal of
volcanology and thermal research , 172, 112-131
44.Rüpke, L., Schmalholz S.M., Schmid, D.W., Podladchikov, Y.Y.
2008. Automated reconstruction of sedimentary basins using twodimensional thermo-tectono-stratigraphic forward models – tested
on the Northern Viking Graben. AAPG Bulletin, 92, 309-326.
45.Røyne, A., Jamtveit, B., Mathiesen, J., Malthe-Sørenssen, A.
2008. Controls on weathering rates by reaction induced hierarchical fracturing. Earth and Planetary Science Letters, 275, 364-369. 46.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.
47.Schmid, D.W., Dabrowski, M., Krotkiewski, D. 2008. Evolution
of large amplitude 3D fold patterns: A FEM sudy. Physics of the
Earth and Planetary Interiors, 171, 400-408.
48.Simon, N. S. C., Neumann, E.-R., Bonadiman, C., Coltorti, M.,
Delpech, G., Grégoire, M., Widom, E. 2008. Ultra-refractory domains in the oceanic mantle lithosphere sampled as mantle xenoliths at ocean islands. Journal of Petrology, 49, 1223-1251.
49.Simon, N. S. C., Podladchikov, Y. Y. 2008. The effect of mantle
composition on density in the extending lithosphere. Earth and
50.Steinberger, B., Torsvik, T.H. 2008. Absoolute plate motions and
true polar wander in the absence of hotspot tracs. Nature, 452,
620-624.
51.Svensen, H ., 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. 52.Torsvik, T.H., 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.
53.Torsvik, T.H., 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.
54.Torsvik, T.H., Steinberger, B., Cocks, L.R.M., Burke, K. 2008. Lonitude: Linking ancient surface to its deep iterior. Earth and Planetary Science letters, 276, 273-282.
55.Van der Straaten, F., Schenk, V., John, T., Gao, J. 2008. Blueschiestfacies redydration of eclogites (Tian Shan, NW-China): Implications for fluid-rock interaction in the subduction channel. Chemical Geology, 255, 195-219.
56.Voisin, C., Grasso, J.-R., Larose, E., Renard, F. 2008. Evolution of
seismic signals and slip papttern along subduction zones: Insights
from a friction lab scale. Geophys. Res. Lett., 35, L08302.
57.Vrijmoed, J. C., Smith, D. C., Van Roermund, H. L. M. 2008. Raman Confirmation of Microdiamond in the Svartberget Fe-Ti type
garnet peridotite, Western Gneiss Region, Western Norway. Terra
Nova, 20, 295-301.
58.Zhijie Xu, Meakin, P. 2008. Phase-field modeling of solute precipitation and dissolution. Journal of Chemical Physics, 129, 014705.
Publications 2009 and in press
1. Angheluta, E. Jettestuen, Mathiesen, J. 2009. Thermodynamics
and roughening of solid-solid interfaces”, Physical Review E (accepted).
2. Austrheim, H., Corfu, F. 2009. Formation of planar deformation
features (PDFs) in zircon during coseismic faulting and an evaluation of potential effects on U-Pb systematics. Chemical Geology
doi:10.1016/j.chemgeo.2008.09.012.
3. Bahr, A., Pape, T., Bohrmann, G., 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.
4. Bjørk, T.E., Mair, K. Austrheim,H. 2009. Quantifying granular material and deformation: Advantages of combining grain size, shape,
and mineral phase recognition analyses. Journal of Structural Geology (accepted).
5. Bonnetier, E., Misbah, C., 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 Physics Journal B, 67, 121-131.
6. Candela, T., Renard, F., Bouchon, M., Brouste, A., Marsan, D.,
Schmittbuhl, J., Voisin, C. 2009. Characterization of fault roughness at various scales: Implications of three-dimensional high resolution topography measurements. Pure and Applied Geophysics
(accepted)
7. de Mahiques, M.M., Wainer, I.K.C., Burone, L., Nagai, R., de Mello
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).
75
8. Ebner, M., Koehn, D., Toussaint, R., Renard, F. 2009. The influence of rock heterogeneity on the scaling properties of simulated
and natural stylolites. Journal of Structural Geology, 31, 72-82.
9. Engvik, A.K., Golla-Schindler, U., Bernd, J., Austrheim, H., Putnis,
A. 2009. Intragranular replacement of chlor-apatite by hydroxyfluor-apatite during metasomatism. Lithos, accepted.
10.Fletcher, R. 2009. Deformable, rigid, and invicid elliptical inclusions in a homogenous incompressible anisotropic viscous fluid.
Journal of Structural Geology, doi:10.1016/j.jsg.2009.01.006.
11.Frehner, M., Schmalholz, S.M., Podladchikov, Y.Y. 2009. Spectral
modification of seismic waves propagating through solids exhibiting a resonance frequency. Geophys. J. Int., 176, 589-600.
12.Galland, O., Planke, S., Neumann, E.-R., Malthe-Sørenssen ,
A. 2009. Experimental modelling of shallow magma emplacement:
Application to saucer-shaped intrusions. Earth and Planetary Science Letters, 277, 373-383.
24.Mazzini, A., Svensen, H., Planke, S, 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.
25.Meakin, P., 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).
26.Milke, R., Abart, R., Kunze, K., Koch-Muller, M., Schmid, D.W., Ulmer, P. 2009. Matrix rheology effects on reaction rim growth I:
evidence from orthopyroxene rim growth experiments. Earth and
Planetary Science Letters, (accepted).
27.Montes-Hernandez, G., Concha-Lozano, N., Renard, F., Quirico, 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.
13.Gisler, G., 2009. Simulations of the Explosive Eruption of Superheated Fluids through Deformable Media. Marine & Petroleum
Geology, in press.
28.Montes-Hernandez, G., Pérez-López, R., Renard, F., Nieto, J. M., Charlet, L. 2009. Mineral sequestration of CO2 by aqueous carbonation of coal combustion fly-ash. Journal of Hazardous Materials, 161, 1347-1354.
14.Gratier, J.-P., Guiguet, R., Renard, F., Jenatton, L., Bernard,
D. 2009. A pressure solution creep law for quartz from indentation experiments, Journal of Geophysical Research, 114,
doi:10.1029/2008JB005652.
29.Neumann, E.-R., Simon, N.S.C. 2009. Ultra-refractory mantle xenoliths 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.
15.Gregory, L.C., Meert, J.G., Bingen, B., Torsvik, T.H., Pandit, M.
2009. Paleomagnetism and geochronology of the Malani Igneous Suite, Northwest India: Implications for the configuration of
Rodinia and the assembly of Gondwana. Precambrian Research,
(in press).
30.Pérez-López, R., Montes-Hernandez, G., Nieto, J. M., Renard, F.,
Charlet, L. 2009. Application of alkaline paper mill waste to reduce CO2 greenhouse gas emissions into the atmosphere. Applied
Geochemistry, /doi 10.1016/j.apgeochem.2008.04.016.
16.Hammer, Ø. 2009. New statistical methods for detecting
point alignments. Computers & Geosciences, doi: 10.1016/j.
cageo.2008.03.012.
17. Hammer, Ø, Dysthe, D.K., Jamtveit, B. 2009.Travertine terracing:
patterns and mechanisms. In: Tufas and Speleothems: Unravelling
the Microbial and Physical Controls. Geological Society of London
Special Publications (accepted).
18.Iyer, K., Podladchikov, Y.Y. 2009. Transformation-induced jointing as a gauge for interfacial slip and rock strength. Earth and
Planetary Science Letters (in press).
19.Jamtveit, B., Putnis, C., Malthe-Sørenssen, A. 2009. Reaction induced fracturing during replacement processes, Contributions to
Mineralogy and Petrology, 157:127-133.
20.John, T., Medvedev, S., Rüpke, L., Andersen, T.B., Podladchikov,
Y.Y., Austrheim, H.O. 2009 Generation of intermediate-depth
earthquakes by self-localizing thermal runaway. Nature Geoscience, 2, 137-140.
21.Lisker, F., John, T. 2008. How much denudation at the Ghana
transform margin? - A review of the offshore apatite fission track
record. Earth Surface Processes and Landforms (Accepted).
31.Quintal, B., Schmalholz, S.M., Podladchikov, Y.Y. 2009. Low-frequency reflections from a thin layer with high attenuation caused
by interlayer flow. Geophysics. In press.
32.Rozhko, A.Y. 2009. Benchmark for poroelastic and thermoelastic numerical orders. Physics of the Earth and Planetary Interiors.
doi:10.10.16/j.pepi.2008.08.016.
33.Sassier C., Leloup, P. H., Rubatto, D., 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]
34.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 Metamorphic Geology, 27, 83-91.
35.Schmidt, A., Weyer, S., John, T., Brey, G.P. 2009. HFSE systematics of rutiles and MORB-type eclogites during subduction: some
insights into Earth’s HFSE budget. Geochimica et Cosmochimica
Acta, 73, 83-91.
36.Skinner, J., Mazzini, A. 2009. Martian mud volcanism: Terrestrial
analogs and implications for formational scenarios. Marine and
petroleum Geology (accepted).
22.Marques F.O., Podladchikov, Y.Y. 2009. A thin elastic core can
control large-scale patterns of lithosphere shortening. Earth and
37.Svensen, H., Planke, S., Polozov, A., 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.
23.Mazzini, A., Nermoen, A., Krotkiewski, M., Podladchikov, Y.Y.,
Planke, S., Svensen, H. 2009. Fault shearing as a mechanism for
overpressure release and trigger for piercement structures. Implications for the Lusi mud volcano, Indonesia. Marine and petroleum
Geology (accepted).
38.Voisin, C., Grasso, J.-R., Larose, E., Renard, F. 2009. Seismic signals and slip patterns down dip subduction zones: insights from a
lab scale experiment. Geophysical Research Letters, 35, L08302,
doi:10.1029/2008GL033356/.
39.Webb, K.E., Hammer, Ø., Lepland, A., Gray, J.S. 2009. Pockmarks
in the Inner Oslofjord, Norway. Geo-Marine Letters DOI 10.1007/
s00367-008-0127-1. 76
Appendices
In books and proceedings
1. Akhmetzhanov, A.M., Kenyon, N.H., Ivanov, M.K., Westbrook,
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.
2. Andersen, H.B., Austrheim, H.O. 2008. The Caledonian infrastructure in the Fjord-region of Western Norway; With special emphasis on the formation and exhumation of high- and ultrahighpressure rocks, late- ot post-orogenic tectonic processes and basin
formation. Excursion guide, 88 pp. 33 IGC excursion NO 29. August 15-22 2008.
3. Cronin, B., Çelik, H., Hurst, A., Gul, M., Gürbüz, K., 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.
4. Røyne, A. Cool Photovoltaics: An experimental study of cooling devices for densely packed photovoltaic arrays under high
concentration. VDM Verlag. ( Dr. Müller, Ed). 2008 (ISBN 9783836480314) 136 p.
4. Feder, J. Self-Affine Dynamics of Stick-Slip Friction. ETH. 28.
January 2008.
5. Feder, J. Structural Phase Transitions in Perovskites, Florida State
University, February 18 2008.
6. Feder, J. Self-Affine Dynamics of Stick Slip Friction, Florida State
University, February 27 2008.
7. Feder, J. Two Phase Flow in Porous and Geological Media, Ecole
Polytechnique, June 26 2008.
8. Feder, J. Dispersion at high and low Peclet numbers, Workshop on
Flow in Porous Media, Brasília, October 20th - 24th, 2008.
9. Feder, J. Extrusion: Plastic Deformation & Friction, Invited presentation Norsk Hydro, June 18 2008
10.Fletcher, R. Grain-scale and macroscopic stress evolution in exhuming rock: fracturing and weathering. The 21 Kongsberg seminar 7-9 May 2008. (Invited talk).
11.Gisler, R.G. Oblique Impacts into Volatile Sediments: Ejection
Distribution Patterns. The 21 Kongsberg seminar 7-9 May 2008.
(Invited talk).
12.Galen R.G. Hydrocode calculations of the generation of tsunamis by landslides with application to La Palma and Åknes, invited
seminar at National Oceanographic Centre, Southampton UK; 7
Feb 2008.
5. Torsvik, T.H., Gaina, C., Redfield, T.F. 2008. Antarctica and Global
Paleogeography: From Rodinia, through Gondwanaland and Pangea, to the birth of the Southern Ocean and the opening of gateways. 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 international symposium on Antarcic Earth Sciences. Washington DC:
The National Academies Press. doi: 10.3133/of2++7-1047.kp11.
13.Galen R. G. Asteroid impacts, tsunamis, and mud volcanos: simulating violent processes in geophysics, invited seminar at Simula
Research Laboratory, Oslo; 29 Feb 2008.
In books and proceedings 2009 and in press
15.Galen R. G. Generation scenarios for Atlantic-region tsunamis:
landslides and volcanos, invited talk at the AGU San Francisco;
15-19 Dec 2008.
1. Bahr, 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. (in press).
2. Gisler, G. 2009. Tsunami generation - other sources, chapter 6 in
The Sea: Volume 15, Tsunamis, edited by Alan Robinson and Eddie Bernard pp 179-200.
3. Gisler, G.R., Weaver, R.P., Gittings, M.L. 2009. Oblique impacts
into volatile sediments: ejection distribution patterns, PARA 08
Conference Proceedings, Trondheim, in press.
4. Torsvik, T.H., Cocks, L.R.M. The Lower Palaeozoic palaeogeographical evolution of the Norteastern and Eastern peri-Gondwana margin from Turkey to New Zealand. J. Geol. Soc. London
Special Publication (in press).
Invited talks 2008
1. Aarnes, I. 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
.
2. Austrheim, H. Zircon coronas around ilmenite – a key to understand the metasomatic and ore forming processes in the KongsbergBamble sectors. Birthday seminar for Else Ragnhild Neumann. The
Academy of Science, Oslo. 28.11.08.
3. Austrheim, H. CO2 sequestration and extreme Mg-leaching in serpentinized peridotite clasts of sediementray basins. Natural History Museum Oslo 12 February.
14.Galen R. G. R. Weaver, M. Gittings, Oblique impacts into volatile
sediments: ejection distribution patterns, invited talk at the PARA
‘08 Meeting, Trondheim; 13-15 May 2008.
16.Jamtveit, B. Reaction assisted fluid migration through rocks. University of München, 25th Jan 2008.
17. Jamtveit, B. Hydration of the Earth’s crust: The role of reaction
driven fragmentation. University of Münster, 5th June 2008.
18.Jamtveit, B. Malthe-Sørenssen, A. Stress generation and hierarchical fracturing in reactive rocks. The 21 Kongsberg seminar 7-9 May
2008.
19.Jøssang, T., Feder, J. Drainage in 2d Systems; Experiments and
simulations. Workshop on Flow in Porous Media, Brasília, October 20th - 24th, 2008.
20.Mathiesen, J. Solid-solid phase transformation and the roughening
of stylolites. The 27th IUGG Conference on Mathematical Geophysics, June 15-20, 2008, Spitsbergen.
21.Mathiesen, J. Morphology studies of desiccation patterns and hierarchical fracture networks. The 21 Kongsberg seminar 7-9 May
2008.
22.Mathiesen, J. Competition between size diffusion and fragmentation: a case study of crystal formation in the Greenland NorthGRIP ice core”. ESF – Workshop on Modelling and interpretation
of ice microstructurs”; Goettingen, April 7. – 12. 2008.
23.Mathiesen, J. Collaboration on Thermo Haline circulation. Niels
Bohr Institute, Cophenhagen, DK; April 22. – 26., 2008.
24.Mazzini. A. Causes and triggers of the LUSI Mud Volcano, Indonesia. Invited speaker at the Dutch Petroleum Geological Society,
The Hague.
77
25.Mazzini. A. Causes and triggers of the LUSI Mud Volcano, Indonesia. Invited speaker at the Wintershall oil company. The Hague
26.Mazzini, A., Svensen, H., Planke, S., Akhmanov, 2008. Causes
and triggers of the LUSI Mud Volcano, Indonesia. In: ”Subsourface sediment remobilization and fluid flow in sedimentary basins”,
21-22 October, London, UK.
27.Mazzini, A., Svensen, H., Planke, S., Akhmanov, 2008. New experiments on LUSI Mud Volcano, Indonesia. LUSI crisis workshop.
27 February, Surabaja, Indonesia.
28.Medvedev S., Hartz E.H., Podladchikov Y. Y., Souche A. Vertical motions of the fjord regions of central East Greenland: Impact
of glacial erosion, deposition, and isostasy. Workshop in Aarhus,
Denmark, 11-12 December, 2008.
29.Meakin, P. Fracture models. The 21 Kongsberg seminar 7-9 May
2008.
30.Neumann, E.-R., Simon, N.S.C. Ultra-refractory mantle in the
oceanic domain. 33IGC, Oslo, 6 14 August. (Keynote talk).
31.Planke, S. The Golden Valley. Birthday seminar for Else Ragnhild
Neumann. The Academy of Science, Oslo. 28.11.08.
32.Raufaste, C., Santucci S. How do the materials flow or break?
French Cultural Center, Oslo, 15-10-2008.
33.Renard, F., Bernard, D. Imaging of a rupture path by X-ray microtomography when hydro-fracturing a porous limestone.
34.Santucci, S. Crackling Dynamics during material failure. HUT,
Helsinki, Finland; April 16.-19. 2008.
35.Santucci, S. Quake catalogs at the laboratory scale. The 21 Kongsberg seminar 7-9 May 2008.
36.Simon, N.S.C. Mantle phase transitions during rifting. EGU, Vienna, Austria, April 13 – 19 2008.
37.Simon, N.S.C. The composition of the mantle lithosphere and how
to make it. Birthday seminar for Else Ragnhild Neumann. The Academy of Science, Oslo. 28.11.08.
38.Svensen, H. New perspectives on large ignons provinces and environmental crises; University Joseph Fourier, Grenoble, France;
January 5 – 8.
39.Svensen, H. Global environmental crises caused by sill emplacement and contact metamorphism in sedimentary basins. PetroBras,
Rio de Janeiro, 26 March 2008.
40.Svensen, H. Sill emplacement and contact metamorphism in the
Vøring Basin during formation of the North Atlantic Volcanic Province 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.
41.Svensen, H. Sill emplacement, contact metamorphism, and gas
venting in the Vøring Basin during formation of the North Atlantic 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.
42.Treagus, S.H., Fletcher, R.C. Controls on folding on different scales
in multilayered rocks. Geological Society of America 2008 Annual
Meeting.
43.Torsvik, T. Fragmentation of continents. The 21 Kongsberg seminar 7-9 May 2008.
44.Torsvik, T. Oslo Hot Spot. Birthday seminar for Else Ragnhild
Neumann. The Academy of Science, Oslo. 28.11.08.
78
45.Vrijmoed, J. C. 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 December 2008.
46.Yarushina V.M. Fluid flow in viscoplastic porous media: porosity
waves as a mechanism for fluid expulsion. Harvard University, Department of Earth and Planetary Sciences and School of Engineering and Applied Sciences.
47.Yarushina V.M. Low-frequency seismic wave attenuation due to
microplasticity in porous media. Boston University, Department
of Earth Sciences.
48.Yarushina V.M. Compaction Driven Fluid Flow in Viscoplastic Porous Media:Porosity Waves as a Mechanism for Fluid Expulsion.
Yale University, Department of Geology and Geophysics.
Talks and posters at conferences 2008
1. Aarnes, I., Podladchikov, Y.Y., Neumann, E.-R. Post-emplacement melt-flow induced by thermal stresses as a feasible mechanism for reversed differentiation in tholeiitic sills. LASI III; 200809-14 - 2008-09-18 (Poster).
2. Aarnes, I., Podladchikov, Y.Y., Neumann, E.-R. Post-emplacement
melt-flow induced by thermal stresses as a feasible mechanism for
reversed differentiation in tholeiitic sills. 33rd International Geological Congress; 2008-08-06 - 2008-08-14 (Poster).
3. Aarnes, I., Podladtchikov, Y.Y., Neumann, E.-R. Post-emplacement melt flow as possible differentiation mechanism in sills. Dave
Yuen’s international 60-birthday symposium; 2008-06-13 - 200806-14 (Poster). 4. Aarnes, I., Svensen, H. Gas formation in contact aureoles: Constraints from kinetic and thermal modeling. LASI III. International
conference, Elba 14-18 September (Talk).
5. Aarnes, I., Svensen, H. Polteau, S. Gas formation from black
shale during contact metamorphism. 33rd International Geological Congress; 2008-08-06 - 2008-08-14 (Talk).
6. Abe, S., Mair, K. How do Things break in Fault Gouge? Abrasion vs. grain splitting in Discrete Element Simulations. European
Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4.
2008 (Poster).
7. Andersen, T.B. 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).
8. Andersen, T.B., Austrheim, H.O., John, T., Medvedev, S. Geology of intermediate to deep earthquakes. Norsk geologisk forening,
avdeling Tromsø; 2008-03-07 - 2008-03-07 (Talk).
9. Andersen, T.B., Austrheim, H.O., John, T., Medvedev, S., Mair,
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 - 2008-0814 (Talk). 10.Andersen, T.B., Mair, K., Austrheim, H.O., Podladchikov, Y.Y.,
Vrijmoed, J.C. The strength of upper mantle peridotite determined
from ultramafic pseudotachylytes. The Kongsberg seminar 7-9 May
2008 (Poster).
11.Andersen, T.B., Mair, K., Austrheim, H.O., Podladchikov, Y.Y.,
Vrijmoed, J.C. The strength of upper mantle peridotite determined
from ultramafic pseudotachylytes. 21st Kongsberg seminar; 200805-07 - 2008-05-09 (Poster).
Appendices
12.Andersen, T.B., Marques, F.O., Schmid, D.W., 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)
13.Angheluta, L. Interface instability driven by a solid-solid phase
transformation, Dynamics Days Delft, 25-29 August 2008 (Talk).
14.Angheluta, L. Roughening of a solid-solid interface: Stability analysis”, Oscarborg student conference 3-4 March 2008 Talk).
15.Angheluta, L. Interface instability driven by a solid-solid phase
transformation. Dynamics Days Delft, August 2008 Talk).
29.Brantley, S., Fletcher, R.C. Relationship between corestone size,
weathering rate, and erosion for a steady state model applied to
natural systems. Goldschmidt conference 2008(Talk).
30.Candela, T., Renard, F., Schmittbuhl, J., Bouchon, M. Roughness
of fault surfaces: implications of high resolution topography measurements at various scales. European Geoscience Union General
Assembly. Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
31.Croizé, D., Bjørlykke, K., Renard, F., Dysthe, D.K., Jahren, J. Pressure-solution in carbonate - An experimental study,. IGC 2008;
2008-08-06 - 2008-08-14 (Poster).
16.Angheluta, L., Jettestuen, E., Mathiesen, J. Interface instability
driven by a solid-solid phase transformation: Roughening of stylolites. The Kongsberg seminar 7-9 May 2008 (Poster).
32.Croizé, D., Bjørlykke, K., Dysthe, D.K., Renard, F., Jahren, J. Deformation of carbonates, experimental mechanical and chemical
compaction. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
17. Angheluta, L., Jettestuen, E., Mathiesen, J. The thermodynamics
and roughening of solid-solid interfaces, 2008 AGU Fall Meeting
(Poster).
33.Dabrowski M., Schmid D.W., Mechanical Anisotropy of a TwoPhase Composite Consisting of Aligned Elliptical Inclusions. Yorsget 1-3 July 2008, Oviedo, Spain. (Talk).
18.Austrheim, H. et al. Fragmentation of olivine and hydration of the
oceanic lithosphere by seismic pumping. The Kongsberg seminar
7-9 May 2008 (Poster).
34.Dabrowski, M. Schmid, D.W.Numerical study of a rigid circular
inclusion in an anisotropic matrix. European Geoscience Union
General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
19.Bachaud, P., Berne, P., Leclerc, J.P., Renard, F. Determination of
the petrophysical characteristics of caprock samples for carbon dioxide storage in deep saline aquifers. European Geoscience Union
General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
35.Dabrowski, M., Hartz, E.H.; Podladchikov, Y. Y.Migmatization
induced overpressure, East Greenland case study. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4.
2008 (Talk).
20.Bachaud, P., Berne, P., 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 International Conference on /Tracers and Tracing Methods/ , 2-6 September 2008, Tiradentes, Brasil. (Talk).
36.Dabrowski, M., Schmid, D.W.; Krotkiewski, M.M. Evolution of
large amplitude 3D fold patterns: a FEM study. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008
(Poster).
21.Beuchert, M.J. & Podladchikov, Y.Y. “Viscoelastic modeling of
mantle convection”. Interdisciplinary Constraints on Solid Earth
th
Dynamics from the Crust to the Core, Dave Yuen’s 60 Birthday
Symposium, Elm, Switzerland, 12-14 june 2008 (Poster).
22.Beuchert, M.J., Podladchikov, Y.Y. & Simon, N.S.C.. Stability of the
Large Low Shear Velocity Provinces (LLSVPs) in the lower mantle.
33rd International Geological Congress, Oslo, Norway, 06-14 august 2008 (Talk).
23.Beuchert, M.J., Podladchikov Y.Y., Simon, N.S.C. Numerical investigation 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).
24.Beuchert, M.J., Podladchikov, Y.Y., Simon, N.S.C., Rüpke, L.H.
Viscoelastic modeling of craton stability. European Geoscience
Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008
(Talk).
25.Beuchert, M.J., Podladchikov, Y.Y., Simon, N.S.C., Rüpke, L.H.
(2008). Viscoelastic modeling of craton stability. Geophys. Res.
Abstr., 10: A-09178.
26.Beuchert, M.J., Simon, N.S.C., Podladchikov Y.Y. Phase Transitions and Thickness of the Oceanic Lithosphere. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4.
2008 (Talk).
27.Bjørk, T.E., K. Mair, H. Austrheim. Quantifying granular material
and deformation: Advantages of combining grain size, shape, and
mineral phase recognition analyses. The Kongsberg seminar 7-9
May 2008 (Poster).
28.Bjørk, T.E., Mair, K., Austrheim, H. Quantifying fault rocks and
deformation: Advantages of combining grain size, shape, and mineral phase recognition analyses.European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
37.Dabrowski, M., Schmid, D.W., Podladchikov, Y.Y. Two-Phase
Composite Subject to Large Deformation: Shape and Mechanical
Anisotropy Development. The Kongsberg seminar 7-9 May 2008
(Poster).
38.Ebner, M., Koehn, D., Toussaint, R., Renard, F., Schmittbuhl, J.
Scaling behavior of natural and simulated stylolites. European
Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4.
2008 (Poster).
39.Fletcher, R.C. Wavelength selection in 3-D decollement folds of
the appalachian Plateau Province with estimates of rheological parameters. Geological Society of America 2008 Annual Meeting
40.Eriksen, O.K. Dysthe, D.K. An experimental study of stylolite formation. The Kongsberg seminar 7-9 May 2008 (Poster).
41.Fristad, K., Svensen, H., Planke, S., Polozov, A.G. Geochemistry 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).
42.Gac, S., Huismans, R., 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.
43.Galerne, C.Y., Neumann, E.-R., Aarnes I., Planke S. Post-emplacement 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).
44.Galerne, C.Y., Neumann, E.-R., Planke, S. 2008. Insights on the
emplacement of saucer-shaped sill complexes from large-scale
geochemical architecture: example of the Golden Valley Sill Comrd
plex, South Africa, (Talk), 33 IGC, Oslo.
45.Galerne, C.Y., Galland, O., Neumann, E.-N., Planke, S. 2008.
What are the feeders of sills? Insights from field observations, geord
chemistry and experimental modeling, 33 IGC, Oslo (Poster).
79
46.Galerne, C.Y., Tantserev, E., Podladchikov, Y.Y., Neumann. E.-R.
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).
47.Galerne, C.Y., Neumann, E.-R., Aarnes, I. 2008. Post-emplacement melt flow in saucer-shaped sills: a mechanism for the generation of S-, D-, and I-shaped compositional profiles, EGU General
Assembly, Vienna (Poster),
48.Galland, O, S. Planke, A. Malthe-Sørenssen, E.-R. Neumann.
Mechanical coupling between magma intrusion and deformation
of country rock: application to dynamic emplacement of saucershaped sills. The Kongsberg seminar 7-9 May 2008 (Poster).
49.Gisler, G. Generation of non-earthquake tsunamis, AGU San
Francisco; 15-19 Dec 2008 (Talk)
50.Gisler, G., Mair, K. Effect of water depth on efficiency of cratering
in crystalline rock with application to the Gardnos impact crater, International Geological Conference, Lillestrøm; August 6 -14
2008 (Poster).
63.John, T., Layne, G., Haase, K. (2008) The chlorine isotope signature of mantle endmembers. Goldschmidt conference. (Talk).
64.Kihle, J., Harlov, D., Jamtveit, B., Frigaard, Ø. SiO2-Al2O3 miscibility at dry granulite facies conditions revealed by formation
of epitaxially exolved quartz inclusions in corundum from a sappirine-garnet boudine, Bamble granulite terrane, SE Norway. The
33rd IGC conference, Oslo, 11 August 2008 (Poster)
65.John, T., Vrijmoed, J.C., 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 Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4.
2008 (Talk).
66.Krotkiewski, M. High performance, large scale computations on
unstructured grids, Notur meeting 2008, Tromsø, Norway, 03.06.
– 05.06. 2008 (Poster)
67.Krotkiewski, M., Dabrowski, M., Y.Y. Podladchikov. Reactive
transport modeling on a modern desktop: resolving versus upscaling. The Kongsberg seminar 7-9 May 2008 (Poster).
51.Gisler, G., Svensen, H., Mazzini, A., Polteau, S., Galland,
O., Planke, S. Simulations of the explosive eruption of supercritical fluids through porous media, EGU Vienna; 13-18 April 2008
(Poster).
68.Krotkiewski, M., Dabrowski, M; Podladchikov, Y.Y. High resolution 3D modeling of heterogeneous parabolic and hyperbolic problems on structured meshes. European Geoscience Union General
Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
52.Gisler, G., Tsikalas, F. Insights into gravitational collapse and
resurge infilling on marine sedimentary-target impact craters revealed by refined numerical simulations of the Mjølnir Crater, International Geological Conference, Lillestrøm; August 6 -14 2008
(Talk)
69.Krotkiewski, M., Podladchikov, Y.Y. Impact of tectonic forces on
clay fluidization and creation of mud volcanos. The Kongsberg
seminar 7-9 May 2008 (Poster).
53.Gisler, G., , Weaver, R., Gittings, M. Oblique impacts into volatile
sediments: ejection distribution patterns, International Geological
Conference, Lillestrøm; August 6 -14 2008 (Talk).
54.Gratier, J.-P., Renard, F., Boullier, A.-M. Evidence of pressure solution processes in the SAFOD 2 samples. EUROPEAN GEOSCIENCE UNION GENERAL ASSEMBLY Vienna, Austria, 13.4.
- 18.4. 2008 (Poster).
55.Hammer, Ø., Webb, K.E. Deflection of oceanic currents in pockmarks. The Kongsberg seminar 7-9 May 2008 (Poster).
56.Huang, H, 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).
57.Huismans, R., 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. SDD01406L.
58.Jamtveit, B., Austrheim, H., Raufaste, C., Røyne, A., MaltheSørenssen, A. Reaction-driven fracturing during replacement processes and metamorphism. AGU Fall meeting, San Fransisco, 15
December 2008 (Talk).
59.John, T., Podladchikov, Y.Y. Drying porosity waves: add fluids to
dry up. The Kongsberg seminar 7-9 May 2008 (Poster).
60.John, T, Podladchikov, Y.Y., Beinlich, A., Klemd, R. (2008). Drying porosity waves: add fluids to dry up. International Geological
Conference no 33. (Talk).
61.John, T, Podladchikov, Y.Y., Beinlich, A, Klemd, R. Drying porosity waves: add fluids to dry up. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).
62.John, T., Layne, G., Haase, K. (2008). The chlorine isotopic composition of mantle endmembers. International Geological Conference no 33. (Talk).
80
70.Lisker, F.; 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 Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
71.Løberg, M., Podladchikov, Y.Y. Compaction-driven fluid flow in
chemically reactive porous media. The Kongsberg seminar 7-9 May
2008 (Poster).
72.Mair, K. Fragmentation in fault zones.The 21 Kongsberg seminar
7-9 May 2008. (Poster).
73.Mair, K., Abe S., 3D numerical simulations of falt zone evolution:
Gouge comminution and strain partitioning. American Geophysical Union Fall Meeting, San Francisco, USA, December 2008.
(Poster).
74.Mazzini, A. Causes and Triggers of the Lusi Mud Volcano, Indonesia. AAPG International Meeting Cape Town, South Africa
(Talk).
75.Mazzini, A. Causes and Triggers of the Lusi Mud Volcano, Indonesia . The geological society Conference: Subsurface sediment remobilization and fluid flow in sedimentary basins, London, UK 19-23
October (Talk).
76.Mazzini, A.: Causes and Triggers of the Lusi Mud Volcano, Indonesia; 2008 AAPG International Meeting Cape Town, South Africa; October 25.-November 1, 2008 (Talk). 77.Mazzini, A., Gisler, G., Krotkiewski, M., Nermoen, A., Podladchikov, Y.Y., Svensen, H., Planke, S., Akhmanov, G.G. Multidisciplinary approach for mud volcano eruptions. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008
(Poster). 78.Meakin, P. Pore scale modeling and simulation of geosystems, US
Department of Energy workshop on Scientific Impacts and Opportunities for Computing, January 10-13, 2008, Maui, Hawaii.
(Oral).
79.Meakin, P. Pore scale simulation of multiphase fluid flow and reactive transport in fractured and porous media.Brown University,
Division of Applied Mathematics, May 1 (2008). (Oral).
Appendices
80.Meakin, P. Research on travertine hot springs at the Center for the
Physics of Geological Processes, University of Oslo. National Science Foundation Chautauqua Workshop, Mammoth Hot Springs,
Yellowstone National Park, Wyoming, July 20, 2008. (Oral).
81.Meakin, P., Huang, H., Malthe-Sørenssen, A. Discrete element
fracture models, Kongsberg Seminar: Kongsberg, May 7-9, 2008.
(Oral).
82.Meakin, P., Huang H., Malthe-Sorenssen, A. Coupling between
fluid generation, fluid flow, deformation and fracturing in porous
media: Discrete element, particle and continuum methods, American Geophysical Union Meeting, San Francisco, Dec 17 2008.
(Oral).
83.Meakin, P. 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).
85.Medvedev, S. Vertical motions of the fjord regions of central East
Greenland: Impact of glacial erosion, deposition, and isostasy (Invited Talk), WORKSHOP: The role of isostasy, climate and erosion
for the evolution of North Atlantic topography , Aarhus, Denmark,
11-12 December 2008 (Talk).
86.Medvedev S, E.H. Hartz, E.H., Podladchikov, Y.Y. Vertical motions of the fjord regions of central East Greenland: Impact of glacial erosion, deposition, and isostasy. The Kongsberg seminar 7-9
May 2008 (Poster).
87.Medvedev, S., John, T., Andersen, T.B:, Podladchikov, Y.Y., Austrheim, H.O. Self-localizing thermal runaway as a mechanism for
intermediate depth earthquakes: numerical studies and comparison with field observations. International Geological Congress no
33; 2008-08-06 - 2008-08-14 (Talk).
88.Montes-Hernandez, G., Charlet, L., 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).
89.Montes-Hernandez, G., Renard, F., Charlet, L. (2008). Ex-situ mineral sequestration of CO2 by aqueous carbonation of alkaline solid
waste, 22^ème RST, 21-24 April 2008, Nancy, France. (Talk).
90.Montes-Hernandez, G., Renard, F., Charlet, L. (2008). Mineral sequestration of CO_2 and removal of dissolved toxic ions by using
aqueous carbonation of lime and/or portlandite, ACEME conference, 1-3 October 2008, Roma, Italy. (Talk).
91.Nermoen, A., Galland, O., Fristad, F., Podladchikov, Y.Y., MaltheSørenssen, A. Experimental modelling of piercement structure formation in sedimentary basins. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Poster).
92.Nermoen, A., Mazzini, A., Gisler, G.R., Krotkiewski, M., Podladchikov, YY., Svensen, H., Planke, S., Akhmanov, G.G. A multidiciplinary approach for mud volcano eruptions - Lusi. Eurpean
Geosciences Union; 2008-04-24 - 2008-04-29
93.Nermoen, A., O. Galland, K. Fristad, Y. Y. Podladchikov, A.
Malthe-Sørenssen, H. Svensen. Experimental constraints on fluidization for the formation of piercement structures in sedimentary
basins. The Kongsberg seminar 7-9 May 2008 (Poster).
94.Neumann, E.-R., Simon, N.S.C. Ultra-Depleted Domains in the
Oceanic Mantle Lithosphere. 33. International Geological Congress; 2008-08-06 - 2008-08-14 (Talk).
95.Neumann, E.-R., Simon, N.S.C. (2008). Ultra-refractory mantle in
the oceanic domain. IGC Abstr. EID05411L.
96.Nicolaisen, F., A. Rozhko, A. Malthe-Sørensen, A. Nermoen.
Simulation of Hydrothermal Vent Complexes. The Kongsberg
seminar 7-9 May 2008 (Poster).
97.Osmundsen, P.T., Andersen, T.B., Braathen, A., Roberts, D.,
Redfield, T.F. Formation and deformation of the Norwegian Òld
Red Sandstone´: an overview. International Geological Congress
no 33; 2008-08-06 - 2008-08-14 (Talk).
98.Polteau, S, Svensen H., Planke S., Aarnes I. (2008). Geochemistry of contact aureoles in the Karoo Basin and the implication for
the Toarcian carbon isotope excursion, IGC 2008 (Talk).
99.Polteau, S, Svensen H., Planke S., Aarnes I. (2008), Geochemistry of contact aureoles in the Karoo Basin and the implication
for the Toarcian carbon isotope excursion, IGC 2008. ((Talk,
H.Svendsen`s workshop).
100.
Polteau S., 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).
101.
Polteau S., Svensen H., Planke S., Aarnes I. (2008), Contact
metamorphism and venting in the Karoo Basin, AGU Fall Meeting, Elkins-Tanton workshop on the Siberian Traps and Mass Extinction (Talk).
102.Polteau, S, Svensen H., Planke S., Aarnes I. (2008) Contact
metamorphism and the global carbon cycle, Eos Trans. AGU,
89(53), Fall Meet. Suppl., Abstract U41B-0018 (Poster).
103.Raufaste, C., 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 Rheology, Palaiseau, France. 20-22 October 2008. (Poster).
104.Raufaste, C., D. K. Dysthe, B. Jamtveit, A. Røyne, J. Mathiesen,
A. Malthe-Sørenssen. Experimental approaches to replacement
processes. The Kongsberg seminar 7-9 May 2008 (Poster).
105.Renard, F. (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).
106.Renard, F., 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 Mécanique des Roches, 23 Octobre 2008. (Talk).
107. Renard, F., K. Mair. Fragmentation, gouge production, and surface roughness evolution on experimentally simulated faults. The
Kongsberg seminar 7-9 May 2008 (Poster).
108.Rüpke, L., Schmid, D., Podladchikov, Y.Y., Schmalholz, Automated thermo-tectono-stratigraphic basin reconstruction - Examples from the Norwegian Sea and North Sea, American Association of Petroleum Geologists, San Antonio (Talk).
109.Rüpke, L.H., Schmid, D.W., Schmalholz, S. M., Podladchikov,
Y.Y. Integrated basin modeling - linking lithosphere and sedimentary basin processes. European Geoscience Union General
Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).
110.Røyne, A., D.K. Dysthe, J. Bisschop.Subcritical cracking in calcite single crystals. The Kongsberg seminar 7-9 May 2008 (Poster).
81
111.Røyne, A., Dysthe, D.K., Bisschop, J., Mechanisms of subcritical cracking in calcite. AGU Fall meeting 15.12. – 19.12.2008
(Poster)
112.Sarwar, M., Santucci, S., Dysthe, D.K., Mair, K. Energy dissipation in a simulated fault system. The Kongsberg seminar 7-9 May
2008 (Poster).
113.Schmid, D., Dabrowski, M., Krotkiewski, M. 3d folding. International Geological Congress Oslo, Norway (Talk).
114.Schmid, D.W.; Abart, R.; Podladchikov, Y.Y.; Milke, R. Matrix
rheology effects on reaction rim growth: coupled diffusion and
creep model. European Geoscience Union General Assembly Vienna, Austria, 13.4. - 18.4. 2008 (Talk).
115.Semprich J., et al. Evaluation of phase transitions in the lower
crust as mechanism for basin formation. The Kongsberg seminar
7-9 May 2008 (Poster). 128.Vrijmoed, J. C., Podladchikov, Y. Y., Andersen, T.B. 2008. An
alternative model for ultra-high pressure in the Svartberget olivine-websterite, Western Gneiss Complex, Norway, Geophysical
Research Abstracts, Vol. 10, EGU2008-A-08915 (Talk).
129.Webb, K.E. Pockmark ecology in fjords and offshore Norway.
The 33rd International Geological Congress, Oslo (Talk). 130.Yarushina, V.M. Interdisciplinary Constraints on Solid Earth
Dynamics from the Crust to the Core: An international Symposium in Honor of Prof. David Yuen’s 60th Birthday; Zurich,
Switzerland. 3.06.-14.06. 2008. (Talk and Poster). 131.Yarushina, V.M. Chimney-like porosity waves as a mechanism
for fluid expulsion at low temperature environments. The International Conference on Mathematical Geophysics CMG2008,
Longyearbyen on Spitsbergen, Norway. 15.06 – 18.06. 2008 (Talk and Poster)
116.Semprich, J., Simon, N. ,Pordladchikov, Y.Y., The effect of pressure, temperature and composition on physical rock properties.
Goldschmidt conference 13.07 – 18.07.2008 (talk)
132.Yarushina, V.M. Microscale yielding as mechanism for low-freth
quency intrinsic seismic wave attenuation. 70 EAGE Conference & Exhibition incorporating Spe Europec 2008, Rome, Italy.
12.06 -14.06. 2008 (Talk and Poster).
117. Semprich, J., Simon, N., Podladchikov, Y.Y. Compression and
subsequent phase transitions as a mechanism for basin formation.
European Geoscience Union General Assembly Vienna, Austria,
13.4. - 18.4. 2008 (Talk).
133.Yarushina V.M. 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
118.Semprich, J., Simon, N.S.C., Podladchikov, Y.Y., Gac, S., Huismans, R. (2008). Evaluation of phase transitions in the lower crust
as mechanism for basin formation. IGC Abstr. MPM11305L.
134.Yarushina V.M., Podladchikov Y.Y. Low-frequency seismic wave
attenuation in porous media due to microscale yielding. 33IGC,
Oslo, 6 - 14 August, (Talk).
119.Simon, N.S.C. (2008). Mantle phase transitions during rifting.
Geophys. Res. Abstr., 10: A-02115 (solicited).
135.Yarushina V.M., Podladchikov Y.Y. Chimney-like porosity waves
as a mechanism for fluid expulsion at low temperature environments. 33IGC, Oslo, 6 - 14 August (Talk).
120.Simon, N.S.C., Podladchikov, Y.Y. (2008). Mantle phase changes, partial melting and subsidence during rifting. IGC Abstr.
STT02708L.
136.Yarushina, V.M., Podladchikov Y.Y. Chimney-like porosity
waves as a mechanism for fluid expulsion. EGU, Vienna, Austria,
April 13 – 19 2008 (Talk).
121.Souche, A., Medvedev, S., Andersen, T.B.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).
137. Yarushina, V.M., Podladchikov, Y.Y. Low-frequency seismic
wave attenuation due to microplasticity in porous media. The
Kongsberg seminar 7-9 May 2008 (Poster).
122.Vrijmoed, J. C., Detailed geological mapping of fragmented ultra-high pressure rocks at Svartberget, West-Norway. Kongsberg
seminar 2008. (Poster)
123.Vrijmoed, J. C., Podladchikov, Y. Y., Andersen, T.B., Corfu, F.,
2008, An alternative model for ultra-high pressure in the Svartberget olivine-websterite, Western Gneiss Complex, Norway,
33th International Geological Congress, 6-14 August, Oslo, Norway. (Talk)
124.Vrijmoed, J. C., Austrheim, H., John, T., Podladchikov, Y. Y.
2008. Metasomatism of the UHP Svartberget olivine-websterite
body in the Western Gneiss Complex, Norway, 33th International Geological Congress, 6-14 August, Oslo, Norway. (Talk)
125.Vrijmoed, J. C., Austrheim, H., John, T., Podladchikov, Y. Y.
body in the Western Gneiss Complex, Norway, Geochimica Et
Cosmochimica Acta, 72, A989. (Talk)
126.Vrijmoed, J. C., Austrheim, H. 2008. Implications of metasomatism for geochronology and P-T estimates: evidence from the
Western Gneiss Region (WGR), Norway, Geophysical Research
Abstracts, Vol. 10, EGU2008-A-09874. (Talk)
138.Ydersbond, Y., D.K. Dysthe. The dynamic brittle-ductile transition in extrusion processes. The Kongsberg seminar 7-9 May
2008 (Poster).
Other talks
1. Aarnes, I. Naturkatastrofer med betydning for vår tid. Fredrikstad
og omegns geologiske forening 3.11.08. Talk.
2. Jamtveit, B. Supervulkaner, Nesbru Rotary Club, Asker, 28 Jan
2008
3. Jamtveit, B. Forskning og administrasjon: Om retning og fart på
et tohodet troll. NUAS (Nordiske universitetsadministratorsamarbeidet) Conferece Blindern, Oslo, 13 June 2008.
4. Jamtveit, B. Om PGP’s aktivitet og samarbeid med institusjoner i
Afrika, Asia, og Latin Amerika. Seminar for ”Nord-Sør utvalget” at
UiO. 26 Aug 2008.
5. Svensen, H. Årsakene til global oppvarming og masseutryddelser
i jordens historie. Norsk geofysisk forenings symposium. Geilo,
Norway, 18 Sept (Invited talk).
127. Vrijmoed, J. C., Austrheim, H., John, T., Podladchikov, Y. Y.
body in the Western Gneiss Complex, Norway, Geophysical Research Abstracts, Vol. 10, EGU2008-A-09457. (Talk)
82
Appendices
In the media 2008
Radio
1. Jamtveit, B. Commenting on the catastrophic 7.9M Earthquake in
China on May 12th, Verdt å vite. NRK Radio P2. May 15, 2008. 2. Mazzini. A. Der Vulkan Lusi auf Java spuckt weiter Schlamm,
Dradio-Deutschlandfunk, 7 May 2008 (interview).
3. Mazzini. A. Radio interview on the BBC Radio 4 about “the Lusi
mud disaster” 23 October 2008 (interview).
4. Svensen, H. Himalayas fjell. Verdt å vite 28.11.08 kl 12:05.
5. Svensen, H. De sub-glasiale Gamburtsevfjellene i Antarktis. Verdt
å vite 4.12.08 Online newspapers and magazines
1. Braeck, S., Podladchikov, Y.Y., Medvedev, S. 2008. Spontaneous
dissipation of elastic energy by self-localasing thermal runaway:
http://arxiv.org/PS_cache/arxiv/pdf/0805/0805.3292v1.pdf
2. Løvholt, F., Gisler, G. Overdreven frykt for LaPalma-tsunamien.
Forskning. No 10.4.08 (Interview).
3. Mazzini. A. Kein Ende der Schlammschlacht, Deutschlandfunk, 7
May 2008 (interview in web article).
4. Mazzini, A. A Wound in The Earth, Time, 28 February 2008 (interview).
5. Mazzini, A. Indonesian mud volcano unleashes a torrent of controversy. News of the Week. 2 February p. 586 (interwiev).
Articles in magazines / books
1. Gisler, G. Violent processes in Geophysics. Meta, 10-13.
2. Hammer, Ø. Livets historie. Geo no. 8 2008, p. 32-35.
3. Jamtveit, B. PGP: et fargerikt fellesskap - til glede for oljeindustrien. Geo p.56-58 October 2008. (Interview)
4. Jamtveit, B. Jordens indre krefter. Geo p44-48, oktober 2008.
5. Jamtveit, B. Jordens indre krefter’, NRK, P2-akademiet, Bind
XXXX, Transit, Oslo, p-114-125. 6. Mair, K. Stanser jordskjelv midt i utviklingen. Nytt fra eVita nr 2,
2008 (interview).
7. Mazzini, A. How to make a volcano. Geoscientist 18. June 2008
(interview).
8. Mazzini, A. An unnatural disaster in Indonesia, Geotimes, August
2008 (interview)
9. Mazzini, A. Indonesian mud volcano may not be man-made, New
Scientist, January 2008 (interview)
10.Mazzini, A. A different kind of eruption wreaks havoc in East Java,
National Geographic, January 2008 (interview).
11.Mazzini, A. Debate over Indonesian mud volcano reignites. The
New Scientist, Volume 200, Issue 2681, 5 November 2008, Page
6.
12.Mazzini, A. Der unendliche Matsch. Süddeutsche Zeitung no 181,
page 16, 2008 (interview).
13.Planke, S. Revealing the secrets of volcanic sedimentary basins.
Geo June 2008, 16-22.
14.Ramberg I.B., Jansen E, Olesen O., 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.
15.Torsvik, T.H. & Steinberger, B. 2008. From continental drift to
mantle dynamics. In ”Geology for Society for 150 Years - The legacy after Kjerulf”, eds. T. Slagstad & R. Dahl. Gråsteinen 12, 24-38.
6. Mazzini, A. Mud eruption ’caused by drilling’. BBC News 1 Nov
2008 (interwiev).
7. Mazzini, A. Geologists blame drilling for Indonesian mud volcano.
Nwe Scientist 31 October 2008 (interwiev).
8. Mazzini, A. What caused the LUSI mud volcano eruption? Innovations report 14.10.2008 (interwiev).
9. Mazzini, A. Indonesian oil company blamed for mud disaster. Enerpub 1 November 2008 (interwiev).
10.Mazzini, A. Experts Clash Over Mud Disaster - Theories on Trigger of Indonesian Mud Volcano. PR Web 22 October (interwiev).
11.Mazzini, A. Two Years On, a Mud Volcano Still Rages--and Bewilders. News of the Week 13 June (interview).
12.Mazzini, A. Unstoppable. Science 13 June 2008 (interview).
13.Mazzini, A. Norwegian researcher studies Lapindo mudflow Indonesia News Blog 27 February (interview).
14.Mazzini, A. Mud volcano cause discussed. AAPG Expolrer, page
32-33.
15.Mazzini, A. AAPG Meeting Pins Mudflow On Drilling. Pesa News
Resourses December 2008/January 2009 (interview).
16.Mazzini, A. Indonesian Mus Flow History. Satnews Daily ¨,December 2008.
17. Mazzini, A. Indonesian oil company blamed for mud disaster. EnerPub 1 November.
18.Mazzini, A. Lapindo Brantas ”responsible” for mud flow. AsiaNews.it, 31 october (interview).
19.Mazzini, A. Experts Clash Over Mud Disaster - Theories on Trigger of Indonesian Mud Volcano. PR Web 22 October.
20.Mazzini, A. Vexing Mud Flow Cause Disputed. Explorer July
2008.
21.Morgan, J. Mud eruption ”caused by drilling” BBC News. (Web
article including interview with A. Mazzini).
Other activities
Newspapers
1. Svensen, H. Dommedag på alvor. Morgenbladet 17 October 2008
(Interview).
2. Lønstad, T. Workshop i ødemarka. (Interview with A. Nermoen
and participants of the PGP thermodynamics course). Oppland
Arbeiderblad 3 November No. 256, page 3.
1. Galland, O., Sassier, C. Andean geotrail 2008-2009
2. Svensen, H. Stand-up researcher during Forskningsdagene at UiO.
In Frokostkjelleren in the old ,central universityi sentrum, 25. september.
83
design by easy.no
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/)
PGP
University of Oslo
PO Box 1048 Blindern
N-0316 Oslo
Norway
phone: (+47) 22 85 61 11
fax: (+47) 22 85 51 01
http://www.fys.uio.no/pgp
[email protected]

Annual Report 2008 PGP

Transcription

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