Aksu Havzası'nın (Antalya, Türkiye) Neojen Stratigrafisi ve Yapısal Unsurları

Öz

Naplı ve bindirmeli Toros kuşağı, Afrika ve Avrasya levhalarının Kretase’den günümüze kadar devam eden yaklaşık K-G yönlü birbirlerine doğru yaklaşma hareketine bağlı olarak oluşmuştur. Bu hareket Neojen’in erken dönemlerinde Isparta Büklümü olarak tanımlanan karmaşık bir morfo-tektonik yapının gelişmesine neden olmuştur. Miyosen’de, Batı ve Orta Toroslar ile Isparta Büklümü’nün iç kesimleri, kırıntılı sedimanlar ve karbonatlarla karakterize edilen denizel havza dolguları ile doldurulmuştur. Çalışma alanı olarak incelenen Aksu Havzası da bu denizel havzalardan biri olup ve Isparta Büklümü’nün tam merkezinde bulunmaktadır. Dolayısıyla, Aksu Havzası Neojen döneminde meydana gelen kabuksal deformasyona ait jeolojik kayıtları tutmuştur. Aksu Havzası dolgusu, genel olarak Orta Miyosen’den Kuvaterner’e kadar denizel kırıntılı karakterde olup; 1 km’den fazla kalınlığa sahiptir. Havzanın Pliyosen öncesi sedimanları yoğun bir deformasyona maruz kalmıştır. Aksu Havzası’nın sedimanter dolgusu temel üzerine uyumsuzluk ile yerleşen Burdigaliyen-Langhiyen Oymapınar Kireçtaşı ile başlar. İstiflenme düzeni, havzanın kuzeyinde ve güneyinde stratigrafik ve litolojik açıdan farklılıklar göstermektedir. Havzanın kuzey kesimindeki Miyosen istifinin en genç birimi Tortoniyen yaşlı olup, Tortoniyen ve Pleyistosen arası birimler birimler eksiktir. Buna karşın, havzanın güneyinde kalan istif nispeten daha tamdır. Litostratigrafik özelliklerin yanı sıra, bu çalışmada Aksu Havzası’nı şekillendiren yapısal unsurlar da ele alınmıştır. Bunlar Aksu ve Kapıkaya bindirmeleri olarak belirlenmiştir. Arazi çalışmalarında yapılan gözlemler ve anahtar fay hatları üzerinden alınan fay-kayma verilerinden elde edilen sonuçlar Aksu Havzasının dört farklı tektonik evrede geliştiğini göstermektedir. Bunlardan ilki, havzanın oluşumu ile ilgili olan ~D-B açılma evresi iken, ikinci evre Isparta Büklümü’nün batı kanadının KD’ya hareketi ile ilişkili olan ~K-G sıkışmalı Likya evresidir. Üçüncü evre, havzada en baskın görülen ~D-B sıkışmalı Aksu evresidir. K-G açılma evresi ise, dördüncü ve son tektonik faz olarak belirlenmiştir. Tüm bu veriler ışığında, Serravaliyen’den Erken Pliyosen’e kadar etkinliğini sürdüren Isparta Büklümü’nün merkezindeki D-B doğrultulu bir kısalmanın varlığı, Afrika ve Avrasya’nın K-G yakınsamasına bağlı levha tektoniği çerçevesinde değerlendirildiğinde ilginçtir. Isparta Büklümü’nün hemen altındaki mantoya ait sismik tomografi görüntüleri Isparta Büklümü’nün altında dalan iki ayrı levha parçasının (Kıbrıs ve Antalya levhaları) varlığına işaret etmişlerdir. Bu durumda, Isparta Büklümü’nün Mio-Pliyosen ve hatta modern dönemdeki evriminde ve Torosların yükselişinde, Antalya Levhası’nın önemli bir katkısı beklenmelidir.

Anahtar Kelimeler

• Aksu Havzası
• Isparta Büklümü
• Kabuk deformasyonu
• Miyosen denizel havzalar

Neogene Stratigraphy and Structural Elements of the Aksu Basin (Antalya, Turkey)

Öz

The Tauride fold and thrust belt formed during ~N-S convergence between African and Eurasian plates since Cretaceous time. This movement led to the development of a complex morpho-tectonic structure, so-called ‘Isparta Angle’ during the early stage of the Neogene time. In Miocene time, the western and central Taurides and the inner part of the Isparta Angle became overlain by marine sedimentary basins which are characterized by clastics and carbonates. Aksu Basin which is determined as study area is one of these marine basins and is located in the center of the Isparta Angle. Therefore, Aksu Basin contains the geological records of the crustal deformation occurred during the Neogene period. The sedimentary infill of the Aksu Basin is mainly characterized by marine clastics with more than 1 km thick from the Middle Miocene to Pliocene. The pre-Pliocene basin infill was subjected to intense deformation. Sedimentary sequence of the Aksu Basin starts with Burdigalian-Langhian Oymapınar Limestone which unconformably overlies the basement unit. The lithostratigraphy in the north is different from that of the south of the basin. The youngest Miocene unit in the north of the basin is the Tortonian aged and the units deposited between Tortonian and Pleistocene is missing in the sequence. On the other hand, the sequence is more complete in the south of the basin. In addition to lithostratigraphic features, the structural elements which are forming the Aksu Basin are also carried out during this study. These are the Aksu and Kapıkaya thrusts. Field observations and results obtained from the kinematic measurements along the key structural zones show that Aksu Basin developed through four different tectonic phases. While the first phase is ~E-W extensional phase which is related to opening of the basin, the second phase is ~N-S compressional Lycian phase. The third phase is ~E-W compressional (Aksu) phase, which is the most prominent phase in the basin. N-S extensional phase is determined as the fourth and the last tectonic phase. Under the light of whole data, presence of the E-W shortening which is active between Serravalian and Early Pliocene in the center of the Isparta Angle is interesting given the plate tectonic setting driven by N-S convergence of the Africa and Eurasia. The seismic tomography images of the mantle below the Isparta Angle indicates that there are two separate slab segments (Cyprus and Antalya slabs). Therefore, an important impact of the Antalya slab should be expected in the Mio-Pliocene and even modern evolution of the Isparta Angle and the uplift of the Taurides.

Anahtar Kelimeler

• Aksu Basin
• crustal deformation
• Isparta Angle
• Miocene marine basins

Kaynakça

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