Framework for cooperation between the built environment department and industry in the area of energy

Research, education and valorization are the three areas on which the strategic plan of Eindhoven University of Technology focuses. The lattermost area concerns the evaluation of knowledge and its successful transfer to the market, through the strengthening of the cooperation with high-tech industry, the support of start-up companies and the establishment of the establishment of an environment in which entrepreneurial spirit may thrive. This report introduces a framework to enable the cooperation between the Built Environment department and industry in the area of energy. Interviews with employees from the department and questionnaires to cooperating companies give an insight into the needs and willingness of each party. The analysis of two case studies of existing relations of the department offers examples and learning points. Combining all these, a value proposition is developed. It includes actions that need to be taken and suggestions in order to improve the quality of the cooperation. Its main aspects include the emphasis on communication and after-care of the projects and on strengthening the link and joining the workforce of the different groups of the department. As a result, a detailed business idea which can support this link is introduced

Monthly migration of a tectonic seismic swarm detected by DInSAR: southwest Peloponnese, Greece

In the period 2011 June–October, a tectonic swarm of nearly 1222 earthquakes occurred in the Messenia prefecture at the southwestern region of the Peloponnese Peninsula. The swarm happened in the Messenia’s Upper Quaternary basin, 25 km NW of the city of Kalamata, and migrated from NNW towards SSE. The largest earthquakes occurred in 2011 August 14 (Mw = 4.8), September 14 (Mw = 4.6) and October 10 (Mw = 4.7), caused moderate structural damages mainly in old houses in four villages and produced particular unrest to the local population. We have investigated the monthly migration of the swarm using Differential Synthetic Aperture Radar Interferometry (DInSAR), presenting for the first time a very close look at the deformation evolution that may reveal an aseismic slip component of the total movement. The geodetically derived slip distribution for the first 4 months revealed that slip migrated laterally along strike (north to south) and vertically from a deep portion, at ∼2.8 km depth, to a shallow portion, at less than 0.5 km, of the fault plane, and concluded its migration towards the surface with a very shallow Mw 4.7 event of 2011 October 10 surprisingly detected by DInSAR

On the Mw 6.4 SW-Achaia (western Greece) earthquake sequence of 8 June 2008: Seismological, field, GPS observations and stress modeling

On 8 June 2008 an Mw(NOA)=6.4 earthquake occurred in NW Peloponnesus, western Greece. This event is the largest strike-slip earthquake to occur in western Greece during the past 25 years. The hypocentre was determined at 18 km depth beneath village Mihoi in SW Achaia. No surface rupture was observed. Many rock falls, slides and liquefaction features have been found as is typical for an earthquake of this size. Double-difference relocations of 370 aftershocks show a linear pattern of events and define a clear NE-SW striking mainshock fault plane. The aftershock region extends approximately 30 km in length, and the width of the surface projection of the aftershocks is as large as 10 km. The depth of the aftershocks rarely exceeds 22 km. Analysis of high-rate GPS data showed that station RLS (Riolos) which is located 12.8 km N5°W of the epicentre was displaced co-seismically 7 mm to the North in agreement with right-lateral kinematics of the rupture. Static (Coulomb) stress transfer analysis indicates loading of faults near the towns of Patras (north) and Amaliada (south), respectively. The earthquake put more emphasis on the role of strike-slip fault in the deformation of western Greece also indicating that seismic strain is partitioned between strike-slip and normal-slip events due to obliquity of the Nubia (Africa) subduction and the N-S extension of the overriding Aegean upper plateSubmitted1.9. TTC - Rete GPS nazionaleJCR Journalreserve

On the Mw 6.4 SW-Achaia (western Greece) earthquake sequence of 8 June 2008: Seismological, field, GPS observations and stress modeling

On 8 June 2008 an Mw(NOA)=6.4 earthquake occurred in NW Peloponnesus, western Greece. This event is the largest strike-slip earthquake to occur in western Greece during the past 25 years. The hypocentre was determined at 18 km depth beneath village Mihoi in SW Achaia. No surface rupture was observed. Many rock falls, slides and liquefaction features have been found as is typical for an earthquake of this size. Double-difference relocations of 370 aftershocks show a linear pattern of events and define a clear NE-SW striking mainshock fault plane. The aftershock region extends approximately 30 km in length, and the width of the surface projection of the aftershocks is as large as 10 km. The depth of the aftershocks rarely exceeds 22 km. Analysis of high-rate GPS data showed that station RLS (Riolos) which is located 12.8 km N5°W of the epicentre was displaced co-seismically 7 mm to the North in agreement with right-lateral kinematics of the rupture. Static (Coulomb) stress transfer analysis indicates loading of faults near the towns of Patras (north) and Amaliada (south), respectively. The earthquake put more emphasis on the role of strike-slip fault in the deformation of western Greece also indicating that seismic strain is partitioned between strike-slip and normal-slip events due to obliquity of the Nubia (Africa) subduction and the N-S extension of the overriding Aegean upper plat

The East Aegean Sea strong earthquake sequence of October?November 2005: lessons learned for earthquake prediction from foreshocks

International audienceThe seismic sequence of October?November 2005 in the Samos area, East Aegean Sea, was studied with the aim to show how it is possible to establish criteria for (a) the rapid recognition of both the ongoing foreshock activity and the mainshock, and (b) the rapid discrimination between the foreshock and aftershock phases of activity. It has been shown that before the mainshock of 20 October 2005, foreshock activity is not recognizable in the standard earthquake catalogue. However, a detailed examination of the records in the SMG station, which is the closest to the activated area, revealed that hundreds of small shocks not listed in the standard catalogue were recorded in the time interval from 12 October 2005 up to 21 November 2005. The production of reliable relations between seismic signal duration and duration magnitude for earthquakes included in the standard catalogue, made it possible to use signal durations in SMG records and to determine duration magnitudes for 2054 small shocks not included in the standard catalogue. In this way a new catalogue with magnitude determination for 3027 events was obtained while the standard catalogue contains 1025 events. At least 55 of them occurred from 12 October 2005 up to the occurrence of the two strong foreshocks of 17 October 2005. This implies that foreshock activity developed a few days before the strong shocks of 17 October 2005 but it escaped recognition by the routine procedure of seismic analysis. The onset of the foreshock phase of activity is recognizable by the significant increase of the mean seismicity rate which increased exponentially with time. According to the least-squares approach the b-value of the magnitude-frequency relation dropped significantly during the foreshock activity with respect to the b-value prevailing in the declustered background seismicity. However, the maximum likelihood approach does not indicate such a drop of b. The b-value found for the aftershocks that followed the strong shock of 20 October 2005 is significantly higher than in foreshocks. The significant aftershock-foreshock difference in b-value is valid not only if the entire aftershock sequence is considered but also if only the segment of aftershocks that occurred within the first 24-h or the first 48-h after the mainshock of 20 October 2005 are taken into account. This difference in b-value should be examined further in other foreshock-aftershock sequences because it could be used as a diagnostic of the mainshock occurrence within a few hours after its generation