Με στόχο τη μελέτη της σεισμικής απόσβεσης στο χώρο του Ν. Αιγαίου καθορίστηκαν τρισδιάστατα μοντέλα απόσβεσης τόσο για τα επιμήκη  όσο και για τα εγκάρσια  κύματα χρησιμοποιώντας τους χρόνους απόσβεσης  που υπολογίστηκαν από τα φάσματα επιτάχυνσης των P και S κυμάτων για σεισμούς ενδιαμέσου βάθους. Για το σκοπό αυτό, χρησιμοποιήθηκαν περισσότεροι από 350 σεισμοί ενδιαμέσου βάθους (εστιακό βάθος μεγαλύτερο των 50km), οι οποίοι είχαν καταγραφεί από δύο τοπικά δίκτυα σεισμογράφων που είχαν εγκατασταθεί στην ευρύτερη περιοχή. Το πρώτο δίκτυο (CYCNET), είχε εγκατασταθεί στην περιοχή των Κυκλάδων (κεντρικό Αιγαίο), ενώ το δεύτερο δίκτυο είχε εγκατασταθεί στα πλαίσια του  προγράμματος  EGELADOS και αποτελούνταν από 65 σεισμογράφους και 24 υποθαλάσσια σεισμόμετρα (OBS) στην ευρύτερη περιοχή της ζώνης κατάδυσης του Αιγαίου. Υπολογίστηκαν οι χρόνοι απόσβεσης  και  ανεξάρτητα της συχνότητας χρησιμοποιώντας δύο τεχνικές. Στην πρώτη προσέγγιση, οι χρόνοι απόσβεσης καθορίστηκαν με αυτοματοποιημένο τρόπο μέσω κώδικα, από την κλίση του φάσματος επιτάχυνσης εξασθένισης της πηγής πάνω από τη γωνιακή συχνότητα θεωρώντας μοντέλο πηγής . Οι υπολογισμοί πραγματοποιήθηκαν στο εύρος συχνοτήτων 0.2-25Hz, χρησιμοποιώντας μόνο τα φάσματα με λόγο σήματος προς θόρυβο μεγαλύτερο από 3, και τα οποία βρισκόταν πάνω από το επίπεδο θορύβου για 4Hz τουλάχιστον για τα P κύματα και για 0.5Hz τουλάχιστον για τα S κύματα. Στη δεύτερη προσέγγιση η επιλογή του τμήματος του φάσματος στο οποίο υπολογίστηκαν οι χρόνοι απόσβεσης γινόταν από το χρήστη. Δημιουργήθηκαν διαγράμματα χρόνου απόσβεσης με την απόσταση αλλά δεν παρατηρήθηκε σημαντική εξάρτηση μεταξύ τους, πιθανότατα λόγω των σημαντικών διαφοροποιήσεων που παρατηρούνται τόσο στη χωρική όσο και σε βάθος κατανομή των τιμών των χρόνων απόσβεσης. Η χωρική μεταβολή των τιμών του  έδειξε ότι οι σταθμοί εξωτερικού τόξου παρουσιάζουν χαμηλές τιμές του  ενώ οι σταθμοί στο πίσω μέρος του τόξου εμφανίζουν σαφώς μεγαλύτερες τιμές. Η παρατηρούμενη αυτή διαφορά γίνεται εντονότερη καθώς το βάθος των σεισμών αυξάνει, ενδεικτικό της τοπικής επίδρασης της υψηλής απόσβεσης (χαμηλό ) της σφήνας του μανδύα πάνω από την καταδυόμενη λιθόσφαιρα, σε συμφωνία με ανεξάρτητες παρατηρήσεις.Πραγματοποιήθηκε τομογραφική αντιστροφή των χρόνων απόσβεσης που υπολογίστηκαν και με τους δύο τρόπους για τη δημιουργία τρισδιάστατου μοντέλου ανελαστικής απόσβεσης στο χώρο του Ν. Αιγαίου ακολουθώντας την προσέγγιση των Papazachos and Nolet [1997a, 1997b], αφού πραγματοποιήθηκε υπολογισμός της πορείας των σεισμικών ακτινών με τη χρήση ενός αλγορίθμου ο οποίος προτάθηκε από τους Moser et al. [1992] ο οποίος βασίζεται στην τεχνική τρισδιάστατης ανίχνευσης των ακτινών και μπορεί να εντοπίζει τις διαθλάσεις τους μέσα από περιοχές χαμηλών ταχυτήτων. Χρησιμοποιήθηκε ένα γραμμικό σύστημα εξισώσεων απόσβεσης που δημιουργήθηκε από ένα τρισδιάστατο κάναβο κόμβων με τρισδιάστατη γραμμική παρεμβολή. Στη συνέχεια με εφαρμογή κατάλληλου κώδικα επιλύθηκε το γραμμικό σύστημα χρησιμοποιώντας τη μέθοδο LSQR [Paige and Saunders, 1982]. Εφόσον το μοντέλο ταχύτητας δεν αλλάζει, άρα δεν αλλάζει και η γεωμετρία των σεισμικών ακτινών, τότε το σύστημα συγκλίνει σε μια επανάληψη (ως γραμμικό) και δεν απαιτείται επαναληπτική διαδικασία με εκ νέου ανίχνευση των σεισμικών ακτινών όπως συμβαίνει στη σεισμική τομογραφία ταχύτητας [Papazachos and Nolet, 1997a]. Με σκοπό την εκτίμηση της αξιοπιστίας των παραγόμενων μοντέλων απόσβεσης πραγματοποιήθηκε εξέταση  της διακριτικής τους ικανότητας  καθώς και εκτίμηση της επίδρασης της ποιότητας των δεδομένων και της παραμετροποίησης του μοντέλου [Kissling et al., 2001]. Για το λόγο αυτό πραγματοποιήθηκαν δοκιμές με τη χρήση συνθετικών χρόνων απόσβεσης χρησιμοποιώντας γνωστά μοντέλα απόσβεσης. Πραγματοποιήθηκαν δοκιμές διακριτικής ικανότητας (resolutions tests) τύπου «σκακιέρας» (checkerboard tests) [Papazachos and Nolet, 1997a; Pozgay et al., 2009; Chen and Clayton, 2012; Lin et al., 2015] κ.α. χρησιμοποιώντας ημιτονοειδής ανωμαλίες για διάφορα μήκη κύματος τόσο στις δύο οριζόντιες διατάσεις όσο και στην κατακόρυφη διεύθυνση, καθώς και δοκιμές με τη χρήση μοντέλων που προσομοιάζουν την πιθανή δομή απόσβεσης της ζώνης υποβύθισης στην περιοχή του Ν. Αιγαίου. Από την αντιστροφή των χρόνων απόσβεσης, και μετά τις δοκιμές διακριτικής ικανότητας, φαίνεται ότι η εντονότερη απόσβεση επικρατεί στην περιοχή κάτω από το ηφαιστειακό τόξο, με τις μεγαλύτερες τιμές ανελαστικής απόσβεσης ( ~300 και  ~200) να επικρατούν στα βάθη των 80-100km, στο ανατολικότερο τμήμα του ηφαιστειακού τόξου όπου και απαντώνται οι σεισμοί ενδιαμέσου βάθους με τα μεγαλύτερα εστιακά βάθη. Η προσδιοριζόμενη αυτή περιοχή υψηλής ανελαστικής απόσβεσης είναι σε εξαιρετική συμφωνία τόσο με την περιοχή χαμηλής ταχύτητας σεισμικών κυμάτων άνω μανδύα από τομογραφικά μοντέλα που έχουν υπολογιστεί με την εφαρμογή διαφορετικών μεθοδολογιών για την περιοχή μελέτης [Drakatos et al., 1997; Papazachos and Nolet, 1997a; Karagianni and Papazachos, 2007], καθώς και με άλλα μοντέλα απόσβεσης που έχουν προταθεί για το Ν. Αιγαίο [Hashida et al., 1988; Kassaras et al., 2008], όσο και με μοντέλα ανελαστικής απόσβεσης που έχουν προσδιοριστεί σε παρόμοιες ζώνες κατάδυσης [Pozgay et al., 2009; Chen and Clayton, 2012; Liu et al., 2014; Liu and Zhao, 2015]. Η προσδιοριζόμενη ζώνη υψηλής απόσβεσης κάτω από το ηφαιστειακό τόξο βρίσκεται σε άμεση εξάρτηση με την κύρια πηγή μάγματος της περιοχής της σφήνας του μανδύα. Η μαγματική αυτή πηγή δημιουργείται από την αφυδάτωση των ένυδρων πετρωμάτων του άνω τμήματος της βυθιζόμενης λιθοσφαιρικής πλάκας της Αν. Μεσογείου, δημιουργώντας την τροφοδοσία μάγματος και τη δημιουργία μαγματικών θαλάμων και ηφαιστείων στην περιοχή του ηφαιστειακού τόξου [Papazachos et al., 2005]. Μετά τον καθορισμό του τρισδιάστατου μοντέλου ανελαστικής απόσβεσης της περιοχής μελέτης του Ν. Αιγαίου με τη χρήση σεισμών ενδιαμέσου βάθους, έγινε η αξιολόγηση του μοντέλου ανελαστικής απόσβεσης σε σχέση με την απόσβεση της ισχυρής σεισμικής κίνησης στο Ν. Αιγαίο. Για να πραγματοποιηθεί η αξιολόγηση αυτή των αποτελεσμάτων της παρούσας διατριβής, πραγματοποιήθηκαν συγκρίσεις με ήδη δημοσιευμένα αποτελέσματα τα οποία αφορούν την απόσβεση των σεισμικών κινήσεων της περιοχής του Ν. Αιγαίου. Επίσης, έγινε σύγκριση των χρόνων απόσβεσης που μετρήθηκαν από τις κλίσεις των φασμάτων επιτάχυνσης (πειραματικά δεδομένα) σε σχέση με το μοντέλο χρόνων απόσβεσης το οποίο προέκυψε από την αντιστροφή. Επιπλέον, υπολογίστηκαν χρόνοι απόσβεσης για διαφορετικά σύνολα και κατανομές σεισμών ενδιαμέσου βάθους που εκδηλώνονται στην περιοχή μελέτης, με εφαρμογή του μοντέλου που προσδιορίστηκε στην παρούσα διατριβή. Από τις συγκριτικές αυτές αξιολογήσεις, επιβεβαιώθηκε η χαρακτηριστική διαφοροποίηση ανάμεσα στους χρόνους απόσβεσης των οπισθότοξων και εξωτερικού τόξου σταθμών, οι οποίες είχαν παρατηρηθεί και στις ισχυρές σεισμικές κινήσεις από τους Skarlatoudis et al. [2013], για τους σεισμούς που συμβαίνουν στο βυθιζόμενο τέμαχος της πλάκας της Αν. Μεσογείου, με τους οπισθότοξους σταθμούς να εμφανίζουν μεγαλύτερους χρόνους απόσβεσης, , ανάλογα με το εστιακό τους βάθος έπειτα από κάποια κρίσιμη υποκεντρική απόσταση ή σε όλες. Οι διαφορές αυτές στους χρόνους απόσβεσης ανάμεσα στους εσωτερικού και εξωτερικού τόξου σταθμούς ήταν παρόμοιες σε όλες τις κατηγορίες σεισμών ενδιαμέσου βάθους της τάξης των ~70-100msec. Σε ότι αφορά τους σεισμούς ενδιαμέσου βάθους που απαντώνται στο όριο διεπαφής των δύο πλακών (Αιγαίου-Αν. Μεσογείου) οι συντελεστές απόσβεσης που υπολογίστηκαν από τους συνθετικούς χρόνους απόσβεσης των εγκαρσίων κυμάτων, για τη συγκεκριμένη κατηγορία σεισμών ενδιαμέσου βάθους, παρουσιάζουν παρόμοιες τιμές με τους συντελεστές απόσβεσης των Skarlatoudis et al. [2013] που υπολογίστηκαν από τη μελέτη των ισχυρών σεισμικών κινήσεων, τουλάχιστον για το εύρος συχνοτήτων 2.5-10Hz.

The study of the anelastic attenuation structure plays a very important role for seismic wave propagation and provides not only valuable constraints for the Earth’s interior (temperature, relative viscosity, slab dehydration and melt transport)  [Stachnik et al., 2004; Pozgay et al., 2009] but also significant information for the simulation of strong ground motions. We examine the attenuation structure of the Southern Aegean area in terms of quality factor (-factor) for both P and S waves ( and ). For this investigation three dimensional P and S wave attenuation models were determined using a large number of  values measured from P and S wave acceleration spectra of intermediate depth earthquakes. More than 350 intermediate-depth events (focal depth above 50km) were employed, recorded by two local networks of portable and permanent instruments installed in the broader area. The first network, CYCNET, was installed in the broader region of Cyclades islands (central southern Aegean sea) while the second one was the large-scale EGELADOS seismic monitoring project, consisting of 65 land stations and 24 OBS recorders in the broader southern Aegean subduction zone. Frequency-independent path attenuation operator  values were estimated from amplitude spectra for P and S waves using two approaches. In the first approach,  was automatically calculated by the slope of the acceleration spectrum, assuming an ω2 source model for frequencies above the corner frequency, .  was measured using only spectra with a signal-to-noise ratio (SNR) larger than 3 for a frequency range of at least 4Hz for P-waves and 1Hz for S-waves in the frequency band of 0.2 to 25 Hz. In the second approach,  values were manually calculated from the linearly-decaying spectra as selected by the user. The observed  data from both approaches were examined against hypocentral distance. No significant linear trend could be observed, most probably because of the significant spatial and depth variations of the anelastic attenuation structure that superimposes the distance effect. The spatial variation of  values for different hypocentral-depth groups was also examined. The obtained results show that fore-arc stations exhibit very low values of , while back-arc stations exhibit much larger values. The observed  fore-arc/back-arc differences becomes more significant as the depth of the earthquakes increases, indicating the effect of the high-attenuation (low-) mantle wedge beneath the volcanic arc. Tomographic inversion, of  values calculated by both approaches (automatic and manual), was applied using the linearized attenuation equations generated for a 3-D node grid with cubic interpolation and a 1-D background velocity model, which was solved by LSQR (Paige and Saunders, 1982). In general, the highest anelastic attenuation with low  and  values is observed for the depths of 50-80km, with the high-attenuation area almost covering the volcanic-arc of the Southern Aegean Subduction. At greater depths low-Q anomalies are localized in the eastern part of the volcanic arc due to the location of the events with depths >100km. Also, a checkerboard resolution test was applied in order to evaluate the resolution of the tomographic images, showing adequate resolution for the largest part of the models and depths up to ~100-120km, as well other resolution tests which resemble the subducting structure. From the tomographic inversion of whole path attenuation operators, it appears that the highest attenuation is observed under the volcanic arc area, with the biggest values   ( ~300 and  ~200) at depths of 80-100km. The high attenuated region is in excellent agreement with tomography studies of seismic velocity produced for the area using different approaches  [Drakatos et al., 1997; Papazachos and Nolet, 1997a; Karagianni and Papazachos, 2007], with attenuation models proposed for S. Aegean [Hashida et al., 1988; Kassaras et al., 2008], as well as with  tomography attenuation models defined for other similar subduction zones  [Pozgay et al., 2009; Chen and Clayton, 2012; Liu et al., 2014; Liu and Zhao, 2015]. The high attenuation zone determined below the volcanic arc is in direct dependence with the main magma source of the area of mantle wedge. This magmatic source, in various depths in the upper mantle, is generated by the dehydration of hydrated rocks at the upper part of the E. Mediterranean subducting slab leading to magmatic chambers and volcanoes  in the area of the volcanic arc [Papazachos et al., 2005].

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