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Figure 1: Map of the Arabian Peninsula. Major tectonic features are indicated. Plate boundaries are indicated by yellow lines. Earthquakes and volcanic centers; shown as red circles and yellow diamond, respectively. Results reveal a splitting time of approximately 1.4 seconds, with the fast axis slightly east of north. The shear-wave splitting results are consistent across the Peninsula, with a slight clockwise rotation parallel for stations near the Gulf of Aqabah. In summary, these results allow us to make several conclusions about the tectonic evolution and current state of the Arabian Plate. Lithospheric thickness implies that thinning near the Red Sea has accompanied the rupturing of the Arabian-Nubian continental lithosphere. The step in the lithospheric thickness across the Shield-Platform boundary likely reveals a pre-existing difference in the lithospheric structure prior to accretion of the terranes composing the eastern Arabian Shield. Tomographic imaging of upper mantle velocities implies a single large-scale thermal anomaly underlies the Arabian Shield and is associated with Cenozoic uplift and volcanism. The Moho and LAB are shallowest near the Red Sea and become deeper towards the Arabian interior. Near the coast, the Moho is at a depth of about 22-25 km. Crustal thickening continues until an average Moho depth of about 35-40 km is reach beneath the interior Arabian Shield. The LAB near the coast is at a depth of about 55 km; however it also deepens beneath the Shield to attain a maximum depth of 100-110 km. These boundary depths are comparable to those at similar distances along profile AA’. At the Shield-Platform boundary, a step is observed in the lithospheric thickness where the LAB depth increases to about 160 km. (Fig.2) 2
Topography, sediment and basement Observed (dots) and predicted (line) gravity anomaly Lithospheric cross-section with shear velocities and densities basement sediment Figure 2: Topography, gravity signature, and lithospheric structure along the Arabian Peninsula. a Topography along the profile plotted with a 32x vertical exaggeration (V.E.). The sediment thickness is shown by the grey shaded areas. b Comparison of the observed gravity data from the GRACE satellites (black dots) and the calculated gravity (grey line) resulting from the structural model shown in c. The S-wave velocities (Vs) in km/s and densities (�) in g/cm3 of each layer are listed (Hansen et al.,2008). References Al-Amri, A. M. (1999). The crustal and upper mantle structure of the Interior Arabian Platform. Geophysical J. International, V. 136, pp. 421 - 430. Hansen, S., Gaherty, J., Schwartz, S., Rodgers, A., and Al-Amri, A. (2008). Seismic Velocity Structure and Depth-dependence of Anisotropy in the Red Sea and Arabian Shield from Surface Wave Analysis. Journal of Geophysical Research, Vol., 113 Doi : 10.1029/2007JB005335. Park Y., Nyblade, A., Rodgers, A., and Al-Amri, A. (2007). Upper mantle structure beneath the Arabian Peninsula and Northern Red Sea from teleseismic body wave tomography: Implications for the origin of Cenozoic uplift and volcanism in the Arabian Shield. Geochem. Geophy. Geosys., 8, doi : 10.1029 / 2006 GC 001566. 3
Page 1: 6 th WORKSHOP of the ILP TASK FORCE
Page 5 and 6: Nr. Prénom NOM Afilation 1 Myqerem
Page 7 and 8: 6th workshop of the ILP Task Force
Page 9 and 10: 11h10-11h30: Vilson Silo, Salvatore
Page 11 and 12: 14h40-15h: Ariana Bejleri, Mensi Pr
Page 13 and 14: ABAZI Sheribane 71 ADDOUM Belkacem
Page 15: ILP TASK FORCE on SEDIMENTARY BASIN
Page 20 and 21: REFERENCES Argnani A., Favali P., F
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Page 56 and 57: This common or different characteri
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Fig. 5: Power Velocity and Cumulati
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Mary FORD ILP TASK FORCE on SEDIMEN
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ILP TASK FORCE on SEDIMENTARY BASIN
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41.5° 41° 40.5° 40° 0 50 km 42
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Results suggest that: a) The incisi
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Uplift of the Gargano Promontory as
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features with a NE-SW shortening di
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interglacial epochs, on which the r
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agreement with the ~E-W extension p
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documented six terrace levels in th
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Koçi R., S Bushati, J.L. Mugnier,
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D e p t h (m) D e p t h (m) NW Shku
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Abstract ILP TASK FORCE on SEDIMENT
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mineralization increase, a reductio
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Besides the hydro-dynamic factors,
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these basins formed. 2) During the
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Adriatic coastline. The alluvial de
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The first project of "Science for P
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Upper Jurassic of the Ionian Zone c
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ock in extension at the relatively
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Fig. 3. In-situ stress measurements
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gneissic) rocks occurred on the nor
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Ionian zones. The thrust belt is ch
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1. In the west: Amonice-Gernec-Gors
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4. A family of four, including all
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The primary purpose of this study i
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Non Clay Minerals present in Brari
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The deformation can be divided in t
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and Italy in the centre, and the Io
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Figure 1 - Geological context (from
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display rapid lateral variations in
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Figure 1 - Geological context of th
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Figure 2 - Example of porosity meas
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as the Dinarides or Hellenides by a
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Ustaszewski, K., Schmid, S.M., Füg
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In new geological map of Albania (i
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1991), Preapulian and Ionian zones
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Attention has been paid in drawing
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Hilterman, F.J., 1983. Seismic lith
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Figure 4. Heavy mineral strata in t
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References Breesch, L., Swennen, R.
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The Pb isotope ratios of all rocks
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Figure 3: Th/Yb versus Ta/Yb plot.
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192
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References � ermák, V., 1993. Li
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Fig. 2 Integrated Strength of the l
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during the flexure of the foreland.
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(iii) to obtain a continuous record
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