13
2 1
4000 m
A Section A A’
Kesme Kőprűçay
Tortonian outlier Figure 1 & 2
Section A: A measured cross section across the Kőprűçay Basin at Kesme. The eastern basin margin has been uplifted and folded during late reactivation of a blind thrust.In the Anamas Dağ, pre-Cambrian basement is thrust over Middle to Late Triassic strata, with a preserved hanging wall anticline. To the south this becomes a blind thrust which underlies the Kirkkavak ridge. A second basement involved thrust runs along the centre of the Kőprűçay valley near Kesme. This thrust also
emplaces pre-Cambrian basement onto Triassic rocks. The fault is covered by undeformed Miocene conglomerates indicating that the fault is at least older than the middle Miocene.
Section A: A measured cross section across the Kőprűçay Basin at Kesme. The eastern basin margin has been uplifted and folded during late reactivation of a blind thrust.In the Anamas Dağ, pre-Cambrian basement is thrust over Middle to Late Triassic strata, with a preserved hanging wall anticline. To the south this becomes a blind thrust which underlies the Kirkkavak ridge. A second basement involved thrust runs along the centre of the Kőprűçay valley near Kesme. This thrust also
emplaces pre-Cambrian basement onto Triassic rocks. The fault is covered by undeformed Miocene conglomerates indicating that the fault is at least older than the middle Miocene.
Peter McPhee
1Douwe van Hinsbergen
1Nuretdin Kaymakci
21Universiteit Utrecht, Netherlands p.j.mcphee@uu.nl 2Middle East Technical University, Ankara, Turkey
The 75km Kirkkavak fault propagation fold which
led to megaslumping in the Miocene Kőprűçay basin
4. Conclusion
Karst Lower to Middle Triassic sandstones and and shales Upper Triassic
limestones Miocene
conglomerate
Miocene outlier (Upper Tortonian)
WEST Looking North EAST
(Road)
Kóprúçay valley
Upper Triassic?
dolomite
Figure 4: Core of the basement anticline on the Kesme – Dumanlı mountain pass. Middle to Lower Triassic sandstones
and shals are exposed in the core of the anticline. On the eastern limb, the Triassic limestone is pervasively dolomitised. An Upper Miocene (Tortonian) outlier is preserved on the eastern side of the fold. The Tortonian sediments onlap onto the
Triassic basement with a dip of around 20 degrees: tilting as a result of late reactivation of the blind fault.
Figure 4: Core of the basement anticline on the Kesme – Dumanlı mountain pass. Middle to Lower Triassic sandstones
and shals are exposed in the core of the anticline. On the eastern limb, the Triassic limestone is pervasively dolomitised. An Upper Miocene (Tortonian) outlier is preserved on the eastern side of the fold. The Tortonian sediments onlap onto the
Triassic basement with a dip of around 20 degrees: tilting as a result of late reactivation of the blind fault.
)
=
)= )
=
)
= )
=
)
= )=
)=
)= )
=
)=
)
= )=
)
=
)=
)=
)
= )
=
)
=
)
=
)=
)=
)
=
)=
)= )=
)
=
)
=
)= )=
)
= )
=
)=
)
=
)= )
=
)
= )=
)
=
Ayanç
Kesme
Bucak Akbaş
Donsuz
Akyaka
İbişler
Dumanlı
Karataş Gaziler
Düzağaç Çukurca
Çaltepe
Karabük
Darıyeri
Zahmadın
Kızıldağ İncedere Güldallı
Darıbükü
Yeşilbağ Kasımlar
Beşkonak
Karabucak Bucakdere
Altınkaya
Pınarbaşı
Kırkkavak
Ballıbucak
Değirmenözü
Eski Beydili Aşağı Kayalar
Köprülü Kanyon
Yukarı Yaylabel
Çimenova (Beydili)
3 1 ° 2 0 ' 0 " E 3 1 ° 1 0 ' 0 " E
3 1 ° 0 '0 " E
37°30'0"N37°20'0"N37°10'0"N
0 2 4 6 8 10
Kilometers
Kirkkavak
Anamas Dag
n A aly t
a N ap p
es
Taur ides
A Section A A’
B Section B B’
Section B: During uplift, the unlithified sand and mud sequence slid
incrementally along the basement-sediment interface. This displacement was accommodated by ductile folding and faulting along the basin axis.
3. Megaslumping
2. Basement Thrusting
Eastward Dip
Steep southward dip Antalya Nappes Quartenary Upper Miocene Middle Miocene Lower Miocene Palaeocen-Eocene Jurassic-Cretaceous Upper Triassic
Middle-Lower Triassic Palaeozoic
Pre-Cambrian
Legend
Figure 3: A basic geological map of the Kőprűçay basin showing key structures. The slump has been shaded to indicate steeply dipping, folded sediments (red), and east-dipping bedding (orange).
Figure 5: Syn-sedimentary and post depositional soft sediment deformation in inter-bedded sandstones and shale in the basin centre.
1. Introduction
We document a major fault propagation fold in the Tauride basement of the Miocene Kőprűçay Basin (Antalya, Turkey). This structure
runs along the eastern side of the Kőprűçay valley and has uplifted the Triassic to Cretaceous basement and Miocene outliers relative to the Miocene basin. Previously, this vertical offset was attributed to strike-slip displacement, or reverse displacement on the Kirkkavak fault: we argue that this fault does not exist as a significant structure.
32°0'0"E 32°0'0"E
31°0'0"E 31°0'0"E 30°0'0"E
37°0'0"N 37°0'0"N
36°0'0"N
Figure 6: Eastern edge of the basin. In the southern half of the valley, a thick succession of conglomerates preserved on the western edge of the basin form a basin margin sequence. A significant margin sequence is not observed along the eastern side of the basin. Minor conglomerates are present, but these are not indicative of a fault scarp of a major fault with more than a kilometre of throw.
In any case, we should expect course clastic sediments to be delivered from the Taurus fold-thrust belt. The lack of marginal facies in the east is either a result of erosional truncation of an uplifted basin flank or a subdued topography in the Taurus.
Figure 6: Eastern edge of the basin. In the southern half of the valley, a thick succession of conglomerates preserved on the western edge of the basin form a basin margin sequence. A significant margin sequence is not observed along the eastern side of the basin. Minor conglomerates are present, but these are not indicative of a fault scarp of a major fault with more than a kilometre of throw.
In any case, we should expect course clastic sediments to be delivered from the Taurus fold-thrust belt. The lack of marginal facies in the east is either a result of erosional truncation of an uplifted basin flank or a subdued topography in the Taurus.
Basal conglomerate
Middle Triassic sandstone and shale Miocene
sandstone and shale sequence
Triassic Dolomite
1. Introduction
5000 m
B Section B B’
Kőprűlu
Isoclinal folding Eroded basin margin
Antalya Nappes AFD deposits
• Shortening in the Taurides fold-thrust belt continued (or restarted) in the Miocene, and did not end in the
Eocene.
• There is no significant evidence of strike-slip deformation along the Kirkkavak ridge. Oblique convergence must be accommodated on other
structures.
• Uplift along the Kirkkavak fold has truncated the basin margin sequence, and caused a major slump to develop in the basin axis.
• Localised variation in the uplift of Miocene sediments is structurally controlled by basement
deformation. In the Taurides, this should be considered when reconstructing the uplift of the Anatolian Plateau using the sedimentary record.
• Shortening in the Taurides fold-thrust belt continued (or restarted) in the Miocene, and did not end in the
Eocene.
• There is no significant evidence of strike-slip deformation along the Kirkkavak ridge. Oblique convergence must be accommodated on other
structures.
• Uplift along the Kirkkavak fold has truncated the basin margin sequence, and caused a major slump to develop in the basin axis.
• Localised variation in the uplift of Miocene sediments is structurally controlled by basement
deformation. In the Taurides, this should be considered when reconstructing the uplift of the Anatolian Plateau using the sedimentary record.
Figure 2: The angular unconformity between the Miocene basal conglomerate and overturned Upper Triassic (Norian-Rhaetian)
limestone. Kesme – Dumanlı mountain pass, Northern Koprűlű valley.
Figure 2: The angular unconformity between the Miocene basal conglomerate and overturned Upper Triassic (Norian-Rhaetian)
limestone. Kesme – Dumanlı mountain pass, Northern Koprűlű valley.
Miocene basal
breccia
WEST Looking North EAST 80o west dip
Megladont bearing Norian-Rhaetian limestones and shales (Overturned!)
72 southeast dipo
Figure 1: Regional geological map of the western Taurus Mts.
(adapted from MTA 1:500,000 Konya sheet).
Figure 1: Regional geological map of the western Taurus Mts.
(adapted from MTA 1:500,000 Konya sheet).
Study Area
Gulf of Antalya
o
o
o o
o
o
o
o
9
26
72
42 90
27
20
79
54 69
15
21
53
14
18
