K–G Gidiflli Aktif Bir Geniflleme Yap›s›, fiuhut (Afyon) Grabeni: Isparta Aç›s›nda Genifllemeli Yenitektonik Dönemin Bafllama Yafl›, GB Türkiye

fiuhut grabeni 8–11 km genifllikte, 24 km uzunlukta, K–G gidiflli, aktif bir geniflleme yap›s› olup, AkflehirAfyon ana grabeninin güney omuzunda ve d›fl Isparta Aç›s›’n›n kuzey uç kesiminde yer al›r. fiuhut grabeni Pliyosen öncesi bir kaya toplulu¤u üzerinde geliflmifltir. Bu kaya toplulu¤u bafll›ca Jura öncesi yafll› metamorfik kayalar, Jura–Alt Kretase yafll› platform karbonatlar›, geç Erken Miyosen–Orta Pliyosen yafll› Afyon volkanik karmafl›¤› ve ayn› yafll› akarsu-göl ortam ürünü volkano-sedimanter bir istiften oluflur. fiuhut grabeninin do¤u kenar› Afyon volkanitleri ve onun örtüsünü oluflturan göl-akarsu ürünü sedimanter bir istif ile flekillenir. ‹yi geliflmifl katmanlanma sunan örtü istifi KKD gidiflli bir seri antiklinal ve senklinal ile deformasyona u¤ram›flt›r. Bu volkano-sedimanter istif BKB–DGD yönlü bir daralma faz›yla deformasyon geçirmifltir. Deformasyon geçirmifl volkano-sedimanter istif Pliyo–Kuvaterner yafll› ve hemen hemen yatay konumlu modern graben dolgusu taraf›ndan aç›l› uyumsuzlukla örtülür. Gerek grabenin en alt dolgusu içinde kay›d edilmifl, gerekse grabeni s›n›rlayan aktif kenar faylar› üzerinde geliflmifl olan kayma vektörlerinin (kayma düzlemi ve kayma çizikleri) eskigerilim analizi, fiuhut grabeninin, DKD–BGB yönelimli bir genifllemenin denetiminde, en Geç Pliyosen’den beri geliflmekte oldu¤unu gösterir. Geniflleme türündeki neotektonik dönem Isparta Aç›s› ve özellikle fiuhut bölgesinde, Geç Pliyosen’de bafllam›flt›r. fiuhut grabeninin tüm kenarlar› bir seri verev at›ml› normal fay seti ve tekil faylar taraf›ndan belirlenmekte ve denetlenmektedir. Çok daha aktif ve büyüklü¤ü Mw=6.3 ve Mw=6.4 aras›nda de¤iflen y›k›c› deprem üretme potansiyeline sahip ana faylar A¤z›kara, Güneytepe, Çobankaya ve Yar›fll› faylar›d›r. Bu durum, özellikle A¤z›kara ve Güneytepe ana faylar›ndan kaynaklanan ve fliddetleri VII-X aras›nda de¤iflen iki y›k›c› tarihsel depremle de (1766 ve 14 Kas›m 1862 depremleri) kan›tlanm›flt›r. Bununla birlikte, Yar›fll› fay›, sismik boflluk özelli¤ini günümüzde de korumaktad›r. Ayr›ca, ince taneli güncel graben dolgusu, yüksek s›v›laflma kapasitesine sahiptir. Bu nedenle, an›lan ana aktif faylar ve s›v›laflma kapasitesi yüksek olan ince taneli gevflek zemin (alüvyon) gerek deprem risk analizinde, gerekse fiuhut ilçesi geliflim planlamas›nda dikkate al›nmal›d›r.

Anahtar Kelimeler:

Isparta Aç›s›, k›vr›m, fiuhut grabeni, verev-at›ml› normal fay; eskigerilim analizi, GB Türkiye

A N–S-trending Active Extensional Structure, the fiuhut (Afyon) Graben: Commencement Age of the Extensional Neotectonic Period in the Isparta Angle, SW Turkey

The Şuhut graben is an 8-11-km-wide, 24-km-long, N-S-trending, active extensional structure located on the southern shoulder of the Akşehir-Afyon graben, near the apex of the outer Isparta Angle. The Şuhut graben developed on a pre-Upper Pliocene rock assemblage comprising pre-Jurassic metamorphic rocks, Jurassic-Lower Cretaceous platform carbonates, the Lower Miocene-Middle Pliocene Afyon stratovolcanic complex and a fluvio-lacustrine volcano-sedimentary sequence. The eastern margin of the Şuhut graben is dominated by the Afyon volcanics and their well-bedded fluvio-lacustrine sedimentary cover, which is folded into a series of NNE-trending anticlines and synclines. This volcano-sedimentary sequence was deformed during a phase of WNW-ESE contraction, and is overlain with angular unconformity by nearly horizontal Plio-Quaternary graben infill. Palaeostress analyses of slip-plane data recorded in the lowest unit of the modern graben infill and on the marginal active faults indicate that the Şuhut graben has been developing as a result of ENE-WSW extension since the latest Pliocene. The extensional neotectonic period in the Isparta Angle started in the latest Pliocene. All margins of the Şuhut graben are determined and controlled by a series of oblique-slip normal fault sets and isolated fault segments. More active faults which are capable of creating destructive earthquakes with magnitudes of Mw=6.3 and Mw=6.5 include the Ağzıkara, Güneytepe, Çobankaya and the Yarışlı faults, as in the occurrence of two devastating historical earthquakes, those of 1766 and 1862, which were seismic events with intensity of VII and X, respectively. The Yarışlı fault, however, still remains seismically inactive. In addition, the finer-grained modern graben infill is thixotropic and so these active faults and the finer-grained alluvial sediments have to be taken into account in both earthquake risk analysis and city planning design in Şuhut County.

Keywords:

Isparta Angle fold, Şuhut graben, oblique-slip normal fault, palaeostress analysis, SW Turkey,

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