Origin of the allochthons in the Lycien belt, Southwest Turkey

Tectonophysics,

361

111 (1990) 367-379

Elsevier Science Publishers B.V., Amsterdam - Printed in The Netherlands

Origin of the allochthons in the Lycien belt, Southwest Turkey &MAIL ijZKAYA Geology Department.

Kuwait University (Kuwait)

(Received June 22, 1989; revised version accepted November 3,1989)

Abstract &kaya, I, 1990. Origin of the allochthons in the Lycien belt, Southwest Turkey. Tectonophysics,

177: 367-379.

The Lycien belt of Southwest Turkey lies between the Menderes metamorphic massif to the northwest and the Bey Daglari carbonate platform to the southeast. The belt is characterized by thrust faults, melanges and peridotites. Strati~ap~c and structural reIations~ps suggest that the ~l~hthons of the Lycien belt were derived from two distinct tectonic terrains. The Koycegiz and ElmaIi thrust dices were from south of the massif; the Tefenni nappe originated far north of the Menderes massif. The latter incorporates platform sediments; melanges and ophiolites represent the edge of a continental platform opening into the Tethys oceanic realm. Correlation of the Elmali and Koyce& thrust slices and autochthonous tectonic elements shows that the Lycien belt between the Menderes massif and the Bey Daglari was a tectonically active zone of weakness. The belt, which may be at the extension of the Ionian zone, was subjected to repeated cycles of deep basin subsidence and intense defo~ation in Triassic, Jurassic-Early Cretaceous and Tertiary times. The Tefemri nappe passed over the Menderes massif and emplaced onto the Lycien terrain in the Late Eocene. The Lycien terrain was subsequently fragmented and overthrusted southeastward onto the Bey Daglari shelf sediments in Late Miocene time.

Introduction

The Lycien thrust fault belt lies between the Menderes metamorphic massif to the northwest (Boray et al., 1973; Durr, 1975; Durr et al., 1978) and the Bey Daglari continental platform to the southeast (Brunn et al., 1971; Gutnic et al., 1979). Large-scale thrust faults involving platform carbonates, pelagic sediments, melanges and a nappe of peridotite characterize the Lycien zone. The origin of the nappes has been a controversial issue. According to Gutnic et al. (1979) and Sengbr and Yilmaz (1981) all the thrust slices have originated from north of the Menderes massif. Poisson (1984) advocated the opposite idea. He claimed that all the thrust slices were derived from the Lycien belt south of the Menderes massif. Our work in collaboration with Turkish PetroDO-1951/90/$03.50

6 1990 - Elsevier Science Publishers B.V.

leum geologists over several years in the Lycien belt showed that two distinct tectonic terranes are represented by the allochthonous thrust slices. One of the terrains was located far north of the Menderes massif. The other terrain was located south of the massif. The northern terrain is represented by the Tefenni nappe, the southern terrane by the Kbyce& Elmali and Tavas thrust slices. Stratigraphy of the tectonic units and their structural ~te~elations~p give clues as to the origin and tectonic setting of the two terrains. The northern terrain was a continental platform which formed the southern border of the Tethys ocean. The southern terrain was a tectonically active belt between the relatively stable Menderes and Bey Daglari continental blocks (Fig. 1). The object of this paper is to present structural and stratigraphic data to demonstrate that there are two distinct

i. 6ZKAVA

368

0 Kizilhisar

Tefenni

I

Marmaris

I Elmali

[

-

-

J

Mediterranean Fig. 1. Location

allochthonous

tectonic

units

in the Lycien

belt.

Another object is to show that a tectonically active strip existed between the Menderes and Bey Daglari. Outline of the geological setting The Lycien

thrust

fault

belt lies between

the

Menderes metamorphic massif to the northwest and the Bey Daglari continental shelf to the southeast (Fig. 2). It is situated the Hellenic Angelier,

Arc-Trench

1979)

along

the extension

system

(Le Pichon

and possibly

constitutes

of and

the east-

ward projection of the Ionian zone (Gutnic et al., 1979). The structure and stratigraphy of the belt has been studied in detail (Graciansky, 1968; Bernoulli et al., 1974; Poisson, 1977). The regional tectonic setting of the belt was outlined by McKenzie (1970) and Dewey et al. (1973). Recent tectonics of the region was studied by McKenzie (1978), Dewey and Sengor (1979), Le Pichon and Angelier (1979) and Angelier et al. (1981). The major structural subdivisions of the belt are: the Bey Da&u-i authochthonous shelf, the allochthonous slices, and the Menderes massif. There are four major allochthonous units which

map of the study area.

are called the Elmali, Kijycegiz, Tavas thrust slices, and Tefenni nappe, respectively, in this communication. A simplified diagram across the belt gives an idea about the geometric relationships of the major tectonic elements in the Lycien belt (Fig. 3). The Tefenm nappe originated Menderes massif and was emplaced time. The amount

of displacement

must be well beyond the width

of the

Kiiycegiz

thrust

Mender-es

massif

Miocene

sediments

north of the in Late Eocene

several

Menderes sheets and

kilometers,

massif.

originated were

of the nappe

hundred

Elmali south

emplaced

of the Bey Daglari

and

of the

onto

the

autochtho-

nous shelf in Late Miocene time. The GGcek tectonic window of the autochthonous shelf sediments is about 70 km west of the Miocene thrust front. The minimum displacement of the Miocene thrust fault is over 100 km in the south. However, this fault disappears north of Burdur. Apparently thrust faulting involved a rotational a pivot located north of Burdur.

motion

around

Stratigraphy of the major tectonic units The stratigraphic sequence of the allochthonous tectonic units provides important clues as to the

ORIGIN

OF THE ALLOCHTHONS

IN LYCIEN

EDITE

Fig. 2. Simplified

geologic

,7 = autochthonous

Bey Daglari

of Tefenni

nappe,

369

BELT, SW TURKEY

RRANE

map

of the Lycien shelf sediments

thrust

fault

belt showing

3 = Elmali thrust

7 = Tavas thrust slice, 8 = Menderes

Fig. 3. Geometric

configuration

of major tectonic

major

tectonic

slice, 4 = KGycegiz thrust massif,

elements

9 = back-thrust

elements,

I = Neogene

slice, 5 = Tefenni

sheets on the Menderes

in the Lycien region,

Southwest

sediment

nappe,

Turkey.

cover.

6 = peridotites

massif.

370

1. OZKAYA

AGE

LITHOLOGY AND FOSSILS Thrust

slices

Mudstone, shale, sandstone, limestone interlayers

Miocene

Argillaceous limestone fossils. Globigerinoides Algal limestones Miolepidocyclina

Eocene

argillaceous

with abundant sp., Globorotalia

with fossils. Miogypsina sp. sp.. Neoalveolina sp.

Thick bedded, fossiliferous limestone Nummulite sp., Alveolina sp.. Globorotalia ep. White thick bedded limestone and Alveolina

Paleocene

sp.

with

with Wiolid

Argillaceous, thin bedded limestone with abundant pelagic fossils, chert nodules and bands. Globotruncana sp.

Upper

White dolomitic

limestone

White limestone

with rudists

r-l

Cretaceous

r 100 50

t Om Fig. 4. Stratigraphicsection of the autochthonousBey Daglari carbonate platform.

origin

and tectonic

evolution

of the terranes

from

which they were derived. The major thrust sheets consist of several imbricate slivers. Each sliver has originated from a different locality and hence display a different stratigraphic sequence. In most cases, the slivers can be reconstructed original tectonic setting with the help

to their of their

stratigraphy. There are some exceptions. For example, the well-known Domuz Dag tectonic unit, which occurs in the northeast of the Lycien belt,

1979), which is regarded as part of the Anatolic microcontinent by $engijr and Yilmaz (1981), or the extension of the Afro-Arabian plate (Ricou, 1980). The Taurid platform displays almost continuous sedimentation since the Cambrian (ezgiil, 1976; Ricou, 1980). Generally, the Paleozoic sediments are discordantly covered by Mesozoic shallow marine carbonates (Kocyigit, 1981). The discordance occurs at the base of the late TriassicLiassic sediments

has defied all attempts to determine its origin until present. A brief description of the representative

stratigraphic

sections

the Taurid

of each tectonic

an upward

structural

unit is provided

here in

succession.

Bey Dag’lari

the

The Bey Daglari area forms Taurid carbonate platform

the extension (Gutnic et

of al.,

and is also recognized

sequence

Only the Upper

of the Kaycegiz

Cretaceous-Tertiary

platform

are exposed

within

the

thrust slice. sediments

within

of

the Bey

Dagari area (Fig. 4). The stratigraphy of the exposed section of Bey Daglari reveal a dominantly carbonate shelf with unconformities before and after the Eocene. There is a slight deepening in Late Cretaceous.

ORIGIN

OF THE

ALLOCHTHONS

IN LYCIEN

AGE

BELT,

371

SW TURKEY

LITHOLOGY AND FOSSILS Tefenni nappe

Chaotic zone Turbidites, basal& red shales, red argillaceous limestone G. Velascoensis, G. Triculinoides

utetian

Thick bedded grey limestone Rugoglobigerina rugosa Globotruncana sp., Heterohelix

‘aleocenelaastrichtian ienomanian Yuronian

sp.

Cream colored thin bedded limestone with chert nodules and bands. Dicyclina sp.. Hedbergella sp., Trinella sp., Heterohelix sp.

3erriasian Calpionella

Alpina 50

Dark grey massive

lurassic

dolomite Om

/ rriassic

Loose red sandstone

Greywacke and shale with basalt limestone blocks

and

Thick bedded alternating dark and light limestones. Glomospira sp., Geinitzina sp., Agathammina sp.

Permian

White massive

dolomitic

limestones

Fig. 5. Nif-Babadag stratigraphicsection of the Kijycegiz thrustslice.

Elmali thrust slice This consists

is structurally mainly

thrust slice. Poisson (1977) reports an authochthonous counterpart of the Yavuz unit on the norththe lowest

of a chaotic

thrust

olistostromal

slice. It deposit

of blocks of Eocene sediments in a elastic matrix of Oligo-Miocene age. There is a relatively undisturbed section of pelagic limestones of Middle Eocene age to the north (see the Yavuz unit of Poisson, 1977). These pelagic sediments correlate well with the Eocene sediments of the Kocegiz

ern extension of the Bey Daglari dur-Isparta region.

within

the Bur-

Kbjicegiz thrust slice This is the second major thrust slice. It rests on the Elmali thrust slice and is overlain by the Tefenni nappe. The main distinguishing character

312

i. 67.KAy~

Micritic limestone with planktonic Globotruncana sp. Rudist limestone Bioclastic

with silicified

fossils

zones

limestone

Radiolarite Pink limestone Nodular pink limestone Limestone with onkolite and algae, chert ? nodules. Involutina liassica Thick bedded grey limestone with chert nodules Paleodasycladus mediterranean

Fig. 6. Kmlcabijliik stratigraphicsection of the KGycegizthrustslice.

of the Kiiycegiz thrust slice is that the sedimentary sequence extends upto the end of the Lutetian. The Kiiycegiz slice displays two distinct stratigraphic

sequences.

Here, the two sections

are de-

present farther up in the sequence. These deep shelf cherty limestones are unconformably overlain by Late Cretaceous-Eocene sediments. The latter consist of reefal limestones at the bottom,

scribed separately. The first section is the composite of Nif and Bababag sections (Fig. 5). The

red micrites, turbidites tostromes with blocks

lower part of the section is from the Nif area, and the upper part is from the Babadag region. The

and basalts

second southeast

section

is from

the lzllcabiiliik

constitute

and basalts on top. Olisof limestones, peridotites the uppermost

part

of the

sequence.

locality

of Tavas (Fig. 6).

Kmlcabb’liik

section

The Kijycegiz tectonic unit out I(lulcabSik, some 50 km southeast

crops at of Tavas

Nif-Babadag section The pre-Jurassic sequence of the Nif-Babadag section consists of Carboniferous shales and limestones, Permian carbonates and Triassic grey-

where the Tavas slice is upthrusted onto the KZjyce&z unit (Fig. 3). The stratigraphic section is presented in Fig. 6. The tivlcabbliik section starts

wackes several

and basalts (Fig. 5). The latter include blocks of Permian limestones and some

with thick-bedded grey limestones with chert nodules of possible Triassic age. The cherty limestones

Triassic quartzites. The greywackes are discordantly overlain by red sandstones of possible Late Triassic-Liassic age. They are overlain in turn by dark dolomitic limestones of Early Jurassic age. Locally, there are also dark grey thick-bedded limestones with chert nodules. Thin-bedded cherty limestones of Late Jurassic-Cretaceous age are

are overlain by cherty limestones, pink limestones marls and radiolarites of Jurassic to possible Early Cretaceous age. The contact is possibly an unconformity. The radiolarites are unconformably overlain by a sequence of bioclastic limestones, rudist limestones, micritic limestones of Late Cretaceous age and red-grey marls and shales of Eocene age.

ORIGIN

OF THE

ALLOCHTHONS

IN LYCIEN

BELT,

AGE Eocene

313

SW TURKEY

~rT~O~OGY AND ---_ ---_

FOSSILS

Grey-pink marls and shales spilite interlayers Olistostome, limestone sandstone, limestone

Paleocene

Limestone

with

breccia,

with hippurites

and rudists

Cretaceous Micritic limestone Jurassic Shaly-sandy

limestone

Triassic

Dark limestone

Permian

White

with chert

crystalline

nodules

limestone 100

F 50

Schists

and quartzites

Om

Fig. 7. Stratigraphic

section of the Tavas thrust slice.

Tavas thrust slice

The Tavas thrust slice, which is sometimes referred to as the “Tavas massif”, lies on the southeastern flank of the Menderes massif. Its relationship with the massif is obscured by the Neogene sediment cover. Close correlation of the Tavas thrust slice with the back-thrust sheets on the southern part of the Menderes massif itself (Caglayan et al., 1980) suggests that it is paraauthochthonous with respect to the rocks of the Menderes. Tavas may be one of the slivers of the southern flank of the Menderes massif, which was backthrusted northwestward onto the massif itself as it was thrusted over the KGyce&iz unit towards southeast. A core of quartz&es, schists and crystalline limestones of possible Paleozoic age, and a cover of carbonates of Mesozoic age constitute the lower

part of the stratigraphic sequence. These rocks are unconformably overlain by Maastrichtian limestones with hippurites, Paleocene limestone breccias and olistostromes, and Eocene red-gray shales, limestones and turbidites (Fig. 7). Further south, around Kale, the Tertiary section includes interlayers of basalts and spilites along with red mudstones and shales. rendered

massif

The Menderes massif consists of a Precambrian continental basement overlain by a cover of Paleozoic-Eocene sedimentary sequence (Boray et al., 1973; Durr, 1975, Akdeniz and Konak, 1979). High-grade metamorphic rocks such as gneiss and ~p~bolites form the core of the massif. The high-grade metamorphic core is warped by Late Paleozoic quartzites and schists and Mesozoic

Allochthonous

Paleocene Maastrich-

?

peridotite

slab

Basalts and shales below, a chaotic mixture of turbidites, limestone and ophiolite blocks above limestone with calcite veins. Globotruncana sigali, Globotruncana lapparanti Red olistostrome Grey olistostrome with limestone serpentine blocks and pebbles

and

Red-grey argillaceous limestone Hedbergella, Globotruncana sp.

Cenomanian

Radiolarite Thin bedded grey cherty, Calpionella Alpina

shaly limestone

Thick bedded, grey limestone nodules and calcite veins

with chert

Massive, white, microscrystalline limestone and dolomite

Fig. 8. Acigol-Inceler stratigraphicsection of the Tefenninappe carbonates.

The

Tertiary

section

sandy-shaly

limestones

and

of Paleocene-Eocene

shales

with a chaotic mixture

and continues of turbidites,

starts

with

as turbidites age and

ends

limestone

and

on the Menderes

the uppermost

ophiolite blocks. The Alpine-stage metamorphism of the massif is attributed by Sengijr and Yilmaz (1981) to the burial of the massif under the load of

are present,

the

within

overriding

thrust

sheets

which

passed

over

Menderes in Late Eocene time. The Menderes massif is considered by these authors as one of the crystalline massifs of Anatolic which constitute the northern part of the Anatolic plate. Tefenni nappe The Tefenni nappe rests on Kiiycegiz and Tavas tectonic units. Outliers of the nappe are presented

massif.

It is thick in the north, The lower thrust succession. Only

but wedges out towards south. plane cuts across the stratigraphic

dotites around slice displays itself.

melange where

Fethiye intense These

and peridotites

it wedges

out under

of the slice the peri-

and Kijycegiz. The Tefenni imbricate thrust faulting imbrications

are partly

the

result of late Cretaceous diastrophism and partly related to the Eocene deformational phase. Different slivers of the Tefenni nappe display variation in stratigraphic sequence. The typical section of the Tefenni nappe, which is presented in Fig. 8, is a composite of Acigol and Inceler sections. The section starts at the bottom with white crystalline massive limestones and dark-gray well bedded cherty limestones and dolomites. These are uncon-

ORIGIN

OF THE

ALLOCHTHONS

IN LYCIEN

formably

overlain

limestones

which grade upward

by

gray

tone-radiolarite-pink quence.

BELT,

thin-bedded

cherty

into a pink limes-

limestone-mudstone

The cherty limestones

alpina indicating

contain

a Berriasian

375

SW TURKEY

se-

Calpionella

age. The pink limes-

tones are overlain by a sedimentary melange which is in turn overlain by a layer of thin-bedded, laminated,

flaggy pink-gray

of Coniacian missing

age.

The

in some localities.

melange the

A younger

spilites

limestone-turbidites,

melange

of

older

is thickest

ages.

that

A common

in all sections

nappe

is tectonically are

in

shallow

turn

is

lationships

sequence

of

nappe

is not related

units

in the region.

age overlies

tectonically

sedimentary

Tavas and Menderes.

north and section is

west. The tectonically

north

little

doubt

genetically units

Structural

re-

tectonic

nappe

overlies

including

Kiiycegiz,

configuration from

of

quence.

the

Bey

carbonates

or deep basinal

ments of Mesozoic age are unconformably lain by a section of Maastrichtian-Lutetian

west of the belt (Fig. 2). These are mainly peridotite tectonites. There are small bodies of gab-

ments.

but

the diabase

dykes,

volcanic

rocks

and

associated pelagic sediments are missing. The volcanic rocks and radiolarites of the Tefenni nappe, which are often Maastrichtian sedimentary

incorporated in the melange, were formed

on deeply subsiding continental platform edges (ozkaya, 1982). The volcanic rocks of Lutetian age of the Kiiycegiz relationship formed

in

Menderes

thrust

slice have no genetic

to the peridotites intraplatform

either.

through

They

south

were of

the

massif.

The stratigraphic and structural relationships indicate that the Lycien belt includes two genetically distinct groups of allochthonous tectonic Similarity

The Maastrichtian-Paleocene

sedioversedi-

part

of the

tectonic units is represented by shallow marine reefal limestones. Eocene sediments which overlie the reefal

limestones

are a volcano-sedimentary

sequence with a chaotic olistostromal zone on top. The Tefenni nappe rests tectonically on the Lutetian section. The stratigraphic sequence of the Kiiycegiz thrust

slice correlates

well with the Tavas

slice. The stratigraphic flank Tavas

sequence

of the Menderes section.

This

massif

suggests

thrust

of the southern is similar

that

the

to the

Koycegiz

slice was originated south of the massif. The Elmali section is well correlated with the marls, shales

Correlation

units.

Daglari,

and Menderes tectonic Mesozoic-Tertiary se-

Ultramafic rocks of the Tefenni nappe cover hundreds of square kilometers south and south-

bros,

far

massif.

sections

shales of Early-Middle

Platform

by

it was derived

Elmali, Kiiycegiz, Tavas, units display a common

age.

peridotites overlain

to other

The structural

overlain by ophiolites which are in turn unconformably overlain by shallow marine limestones and Eocene

is

that the Tefenni

The Tefenni

of the Menderes

Stratigraphic

by

evidence

that

aspect

the sedimentary

carbonates.

all other

from

to the Tefenni

unconformably

also provide

The

leaves

belong overlain

marine

melange

and becomes

stratigraphic

which

of

different

Maastrichtian-Paleocene

melange which

stratigraphy

is fundamentally

sedimentary

in the southeast

thinner towards the Maastrichtian-Paleocene

Cretaceous-Tertiary nappe

and

of Maastrichtian-Paleocene?

sediments

Late

the other units.

Eocene

limestone-mudstones

sedimentary

The

the Tefenni

of the

Tertiary

sediments

and

sedimentary melange of the Kiiycegiz slice with the Maastrictian-Paleocene sediments and melange of the Tefenni slice prevented early workers from recognizing the presence of two distinct tectonic units in the region with represent two entirely different tectonic terranes.

and turbidites of the Paleocene-Eocene section of the Kiiycegiz thrust slice. Presence of authochthonous counterparts of the Koyce$jiz and Elmali sequence in the northern extension of the Bey Daglari

platform

around

Homa (see 6zti.irk,

1981;

Koqyigit, 1984) and the Barla-Isparta region (see Gutnic et al. 1979) shows that the Kiiycegiz slice is the extension of the Bey Daglari shelf itself. The relationship of the Menderes massif with the Taurid platform is not well established. Platform carbonates on both of these and especially the presence in both regions of a bauxite horizon within the Jurassic-Cretaceous limestones suggest

376

1. OZKAYA

NW

Fig. 9. Schematic

Tavas

geologic

Tavas and KGyc&iz

thrust

slices, 4 = sediments

cross-section

of the Lycien belt. I = metamorphic

slices, 3 = Paleocene-Middle of the Tefenni

nappe,

Eocene

5 = opbioiites

some close correlation (Gutnic et al., 1979). It should be noted that the same bauxite horizon also occurs within the limestones of the Kliycegiz slice. Stratigraphic correlation and structural configuration (Fig. 9) strongly suggest that the Kiiycegiz and Elmali thrust slices were derived from a tectonic terrain south of the Menderes massif. The terrain was located between Menderes to the northwest and Bey Daglari to the southeast. Regionally, the Bey Da&& platform corresponds to Geyikdagi unit, and the Tefenni nappe to the Bozkir unit of 6zgiil (1984). The regional correlation of the Kiiycegiz and Elmali and Tavas thrust sheets is not very clear, but if the Tavas tectonic unit corresponds to the Bolkar Dag units of the Ala Da& then the Ksycegiz and Elmali thrust sheets are allochthonous equivalents of the Geyikdagi unit. The Paleocene-Eocene trough along the Lycien belt, which is characterized by red marls, turbidites and basic volcanism may be equivalent to 6zgiil’s Dipsizgol basin and the Maden basin of Southeast Turkey (Perincek and Kozlu, 1984). Geologic history Tectonic setting of the Tefenni nappe was at the northern edge of a continental platform bordering the Tethys ocean. Deep subsidence of the platform edge in Jurassic-Cretaceous times was followed by ophiolite abduction at the end of the Cretaceous. The ophiolites originated in the Tethyan oceanic realm far north of the Menderes

twbidites,

rocks of Paleozoic

age, 2 = Mesozoic

carbonates

red shales and spilites of the Tavas and Koycegiz

of the Tefenni

nappe,

6 = sediments

of the thrust

of the Elmali thrust slice.

massif (Gutnic et al., 1979). Subsequently, shallow marine limestones of Eocene age were unconformably deposited over the ophiolites during a quiet period before the major Late Eocene diastrophism. The platform was shattered and slices were displaced, with ophiolites on their back southward over the Menderes massif onto the Lycien belt in Late Eocene time. The Elmali, Kaycegiz and Tavas units are basically slivers of sediments of a tectonic terrain which was located south of the Menderes massif, between the massif and the Bey Daglari autochthonous carbonate platform farther to the southeast. The thrust sheets are stacked in such a manner that each slice was derived from sources successively north of the slice underlying it. When the Menderes, Tavas, Kijycegiz and Elmali tectonic units are restored palinspastically, the following picture emerges. A tectonically active zone between two continental platforms existed in southwest Turkey from at least as early as TriassicMiocene. This is evidenced by the repeated subsidence and deformation of the area represented by KiSyce&z and Elmali thrust slices in contrast to the persistently stable shelf characteristics of the Menderes and Bey Daglari areas. Triassic sediments of the Bey Daglari to the southeast, Tavas and Menderes to the northwest are shelf carbonates. The Triassic of the NifBabadag section of the Kijyce&z thrust slice consists of turbidites, and basalts which occur as a chaotic melange with huge limestone and quartzite blocks. This signifies the rifting attempt along the Lycien belt in the Triassic. The Late Triassic-Li-

ORIClN

OF THE ALLOCHTHONS

IN LYCIEN

377

BELT, SW TURKEY

NW +--

Bey doglarl

Menderes

cl

---+

SE

------.A. b,

.

-

-c

Miocene

a/

Lots Eocene

Paleocene-Middle 9

I

9

I

I

9

Eocene

I

9

I

9

Late Cretaceous

Jurassic-Lower

1.

.

/I\

/I\

Cretaceous

/I‘\

/I

Jurassic

I

I

I

I

I

Triassic

I

,..,..:,y:..... ;..., ...

I

I

I

I Triassic I/

Fig. 10. Cartoon showing geologic evolution of the Lycien belt. I = Permian shelf carbonates, 2 = Triassic carbonates, 3 = turbidites, Cretaceus shallow shelf 4 = Jurassic carbonates, 5 = Jurassic-Lower Cretaceous deep shelf carbonates, 6 = Jurassic-Lower carbonates, 7 = Upper Cretaceous shallow marine carbonates, 8 = Palette-Middle Eocene red marls and shales, 9 = PaleoceneMiddle Eocene shallow marine carbonates. (I = Tefenni nappe, b = Kiiycegiz thrust slice, c = Elmah thrust slice.

assic unconformity between the underlying Triassic melange and overlying Early Jurassic shelf carbonates reflect the end of the Early Triassic rifting and transformation of the region into a shelf. Shallow marine platform carbonates constitute the bulk of the Triassic-Lower Cretaceous section in Bey Daglari, Tavas and Menderes terrains. The Nif-Babadag section of the Kbycegiz thrust sheet includes cherty micritic limestones of relatively deeper en~ro~ent. The Ktvlcabiiliik section of the same thrust sheet with pelagic limestones and radiolarites indicates past-existence of a deep trough in the Jurassic between Menderes and Bey Daglari terrains. During the Late Cretaceous

there was a shallow marine environment throughout the region, but starting from the Paleocene until the end of the Middle Eocene a deeply subsiding through was regenerated between the Menderes and Bey Daglari terrains. This is evidenced by the Lutetian turbidites, the red pelagic limestones-spilite section and the sedimentary melange of the Koycegiz, Elmali and Tavas thrust sheets. The Kiiycegiz and Elmali thrust sheets were thrust faulted southeastward onto the Miocene elastic sediments of the autochthonous Bey Daglari shelf region towards the end of the Miocene. The Koycegiz thrust slice carried the Tefenni nappe on

1. OZKAYA

378

its back, Eocene.

which

has been

A cartoon

tory of the Lycien

emplaced

which depicts

in the Late

the geologic

belt is presented

his-

the Exploration

Group

who shared

with me their

ideas and information.

in Fig. 10. References

Discussion

and conclusion Akdeniz,

The

presentation

portant

points.

thrust

are

emphasizes two

sheets which represent

terrains,

respectively

Menderes from

above

There

massif.

an active

Tethys

The Tefenni

realm

massif. The Kiiycegiz, fragmented

and

Lycien tectonic the Menderes Bey Daglari Tefenni

terrain

margin

Elmali

of

tectonic

south

nappe

far north

thrust

of

the

was derived bordering

the

of the Menderes

and Tavas slices are

faulted

remnants

of the

which was located

south of

massif, between the massif and the platform farther southeast. The

nappe

evolution

and

im-

groups

two distinct

north

continental

oceanic

two

main

bears

of an active

evidence

of

continental

the

tectonic

margin.

Deep

subsidence of the margin in Jurassic time was followed by volcanic activity, sedimentary melange accumulation and finally emplacement of ophiolites at the end of the Cretaceous. A brief stable period

of shallow

seas in the Eocene

was followed

by breaking up of the continental subsequent emplacement of platform

margin and slivers with

ophiolites toward the south. The study also reveals that the Lycien was a tectonically

active

belt between

N. and Konak,

dolayindaki

kaya

kayalarin Angelier,

konumu.

nisms

and

Bernoulli,

southeastern

Menderes

masifinin

J.H.,

Juteau, Outline Explor.

Sot.

the stable

continental blocks of the Menderes massif and the Bey Daglari platform at the extension of the Ionian zone. The belt may represent a fracture zone between the Menderes and Bey Daglari continental blocks, which was activated repeatedly during periods of major plate adjustment. Indeed, the main stages of tectonic activity in Triassic, Late Cretaceous, Eocene and Miocene times coincide with major changes in relative motions of the African-Arabian and Asian plates (Dewey et al., 1973).

P., 1974.

Turkey)

The

into

the

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