Tectonostratigraphic Evolution of the North Anatolian Palaeorift

23 Pages·2003·0.39 MB·Turkish

Turkish Journal of Earth Sciences(Turkish J. Earth Sci.), Vol. 11,2002, pp. 169-191.Copyright 'T(cid:134)B(cid:220)TAK
Tectonostratigraphic Evolution of the North Anatolian
Palaeorift (NAPR): Hettangian—Aptian Passive Continental
Margin of the Northern Neo-Tethys, Turkey
AL(cid:220) KO(cid:130)Y(cid:220)(cid:218)(cid:220)T1& DEM(cid:220)R ALTINER2
1 Tectonic Research Unit, Middle East Technical University, Department of Geological Engineering,
TR-06531 Ankara, Turkey (e-mail: [email protected])
2 Marine Micropaleontology Research Unit, Middle East Technical University,
Department of Geological Engineering, TR-06531 Ankara, Turkey
Abstract:The Jurassic-Early Cretaceous stratigraphical, sedimentological and structural evolutionary history of the
northern branch of Neo-Tethys is recorded and preserved within an average 6-km-thick basin fill. The basin fill is
well—exposed as discontinuous inliers of varying size and thickness within, and to the north of, the Late
Cretaceous—Early Tertiary (cid:220)zmir-Ankara-Erzincan Suture throughout northern Turkey.
This basin fill unconformably overlies a substratum comprising the deformed rock assemblages of the Triassic
Karakaya palaeorift and its Hercynian basement. Detailed studies based on geological mapping at a 1/25,000 scale
and stratigraphic sections measured at 14 type localities show that this infill includes stratigraphical and
sedimentological key units, which comprise a 0.1—3.8-km-thick basal association (proto- and syn-rift infill), a
0.1—1.5-km-thick platform association, a 1.6-km-thick basinal association (transitional to post-rift stage infill), and
syn-depositional megabreccias and slumps. This basin fill is shaped by a series of structural units which result from
four distinct phases of extensional faulting. These structural units comprise interior grabens, subplatforms,
platforms, palaeohighs, rift-related unconformities (proto-, syn- and post-rift unconformities) and rift-related
faults. The latter include older growth faults, inner and outer master fault systems, and a marginal fault complex.
This thick Jurassic-Lower Cretaceous basin fill has been interpreted to be the product of a palaeorift,
designated here as the north Anatolian palaeorift (NAPR). The young substratum and the key stratigraphical and
structural elements support the interpretation that the NAPR comprised the south-facing passive continental
margin of north Neo-Tethys in northern Turkey. It had the character of a supradetachment basin and can be
explained by the evolution of a three-stage graben model during the Hettangian-Aptian time interval.
Key Words: tectonostratigraphy, palaeorift, three-stage graben model, supradetachment basin,
Hettangian—Aptian, northern Neo-Tethys, Northern Turkey
Kuzey Anadolu Paleoriftinin (KAPR) Tektonostratigrafik Evrimi:
Kuzey Neo-Tetiz(cid:213)in Hettanjiyen—Apsiyen Pasif K(cid:221)ta Kenar(cid:221), T(cid:159)rkiye
(cid:133)zet: Neo-Tetiz(cid:213)in kuzey kolunun Jura—Erken Kretase(cid:213)deki stratigrafik, sedimentolojik ve yap(cid:221)sal evrimi 6 km
kal(cid:221)nl(cid:221)(cid:219)(cid:221)ndaki bir havza dolgusu taraf(cid:221)ndan kay(cid:221)d edilmi(cid:223) ve korunmu(cid:223)tur. Bu istif, kuzey T(cid:159)rkiye boyunca yer alan
Ge(cid:141) Kretase—Erken Tersiyer ya(cid:223)l(cid:221) (cid:220)zmir-Ankara-Erzincan kenedi i(cid:141)inde ve onun kuzeyinde, de(cid:219)i(cid:223)ik boyut ve kal(cid:221)nl(cid:221)kl(cid:221)
s(cid:159)reksiz a(cid:223)(cid:221)n(cid:221)m pencereleri olarak y(cid:159)zeyler.
Jura—Kretase ya(cid:223)l(cid:221) havza dolgusu daha ya(cid:223)l(cid:221) bir temel (cid:159)zerinde uyumsuz olarak yer al(cid:221)r. Bu ya(cid:223)l(cid:221) temel, Triyas
ya(cid:223)l(cid:221) Karakaya paleoriftinin deformasyon ge(cid:141)irmi(cid:223) kaya toplulu(cid:219)undan ve riftin Hersiniyen ya(cid:223)l(cid:221) temelinden olu(cid:223)ur.
1/25,000 (cid:154)l(cid:141)ekli jeolojik haritalama ve 14 tip alanda (cid:154)l(cid:141)(cid:159)len stratigrafik kesitlere dayal(cid:221) ayr(cid:221)nt(cid:221)l(cid:221) (cid:141)al(cid:221)(cid:223)malar, havza
dolgusunun, (cid:154)nemli baz(cid:221) stratigrafik ve sedimentolojik anahtar birimler i(cid:141)erdi(cid:219)ini g(cid:154)stermi(cid:223)tir. Bu anahtar birimler
ba(cid:223)l(cid:221)ca 0.1—3.8 km kal(cid:221)nl(cid:221)kta taban toplulu(cid:219)u (rift (cid:154)ncesi-riftle ya(cid:223)(cid:221)t dolgu), 0.1—1.5 km kal(cid:221)nl(cid:221)kta platform
toplulu(cid:219)u, 1.6 km kal(cid:221)nl(cid:221)kta havza toplulu(cid:219)u (ge(cid:141)i(cid:223) evresi-rift sonras(cid:221) dolgu), depolanma ile ya(cid:223)(cid:221)t megabre(cid:223)ler ve
oturma-y(cid:221)k(cid:221)lma yap(cid:221)lar(cid:221)ndan olu(cid:223)maktad(cid:221)r. Havza dolgusu, d(cid:154)rt ayr(cid:221) normal faylanma evresinde geli(cid:223)mi(cid:223) bir seri
yap(cid:221)sal birim taraf(cid:221)ndan (cid:223)ekillenmi(cid:223)tir. Bu yap(cid:221)sal birimler ba(cid:223)l(cid:221)ca i(cid:141) graben, ikincil platform, platform,
paleoy(cid:159)kselti, rift uyumsuzlu(cid:219)u (rift (cid:154)ncesi, riftle ya(cid:223)(cid:221)t ve rift sonras(cid:221) uyumsuzluklar) ile rift faylar(cid:221)ndan olu(cid:223)ur. Rift
faylar(cid:221) b(cid:159)y(cid:159)me faylar(cid:221), i(cid:141) ve d(cid:221)(cid:223) graben ana fay sistemleri ve kenar fay komleksleriyle temsil edilir.
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NORTHANATOLIAN PALAEORIFT
6 km kal(cid:221)nl(cid:221)ktaki Jura—Erken Kretase ya(cid:223)l(cid:221) bu havza dolgusu, Kuzey Anadolu paleorifti (KAPR) olarak adlanan
bir paleoriftin (cid:159)r(cid:159)n(cid:159) olarak yorumlanm(cid:221)(cid:223)t(cid:221)r. Gerek havza temeli gerekse havza i(cid:141)inde geli(cid:223)mi(cid:223) stratigrafik ve yap(cid:221)sal
birimler, Kuzey Anadolu paleoriftinin, kuzey T(cid:159)rkiye(cid:213)de, Neo-Tetiz(cid:213)in g(cid:159)neye bakan pasif k(cid:221)ta kenar(cid:221)n(cid:221) olu(cid:223)turdu(cid:219)u
yorumunu desteklemektedir. KAPR, s(cid:221)yr(cid:221)lma fay(cid:221) (cid:159)zerinde geli(cid:223)mi(cid:223) bir havza karakterine sahip olup, bu havzan(cid:221)n
evrimi, Hettanjiyen—Apsiyen s(cid:221)ras(cid:221)nda etkin olmu(cid:223) (cid:159)(cid:141) evreli bir graben modeli ile a(cid:141)(cid:221)klanabilir.
Anahtar S(cid:154)zc(cid:159)kler: tektonostratigrafi, paleorift, (cid:159)(cid:141) evreli graben modeli, s(cid:221)yr(cid:221)lma fay(cid:221) (cid:159)zeri havza,
Hettanjiyen—Apsiyen, Kuzey Neo-Tetiz, kuzey T(cid:159)rkiye
Introduction of the Northern Neo-Tethys, which began to develop by
rifting during the Hettangian in the back-arc setting of
The past decade has produced a revolution in basin
the southerly subducting Palaeo-Tethys ((cid:222)eng(cid:154)r 1979).
analysis. This revolution resulted from both the
Sedimentological evidence for the opening history of the
recognition of highly extended terrains, and the
northern branch of Neo-Tethys and its Late
development and refinement of some analytical
Jurassic—Aptian evolution in north-western Anatolia have
techniques such as numerical modelling, isotope
been previously documented by G(cid:154)r(cid:159)r et al.(1983) and
stratigraphy, improved geochronology, magneto-
Ko(cid:141)yi(cid:219)it et al.(1991a).
stratigraphy and multi-channel seismic data. These
advances have facilitated a distinction between traditional In the present paper we discuss and summarize the
rift basins and supradetachment basins (Friedmann & key structural elements and tectonostratigraphic
components of the NAPR based mainly on field data
Burbank 1995).
obtained throughout northern Turkey from Hal(cid:221)lar in the
The African rift system, Gulf of Suez, northern Red
west to Yusufeli in the east (Figure 1). In addition, special
Sea, the Newark rift system and Lake Baikal are all
attention is focused on the tectonostratigraphic
examples of classical rift basins (Hempton 1987; Morley
characteristics of the intra-carbonate platform
1989; Leeder 1995). They developed within
palaeohighs. Detailed 1/25,000 scale geologic maps and
intracontinental terrains such as the main continental bulk
the measured sections showing the different lithofacies,
of the African plate and remote from young orogens.
synsedimentary structural elements, such as growth
Therefore, they are associated with normal-thickness,
faults, slumps, slope breccias, olistostromes; grabens and
cold and old lithosphere, and are characterized by alkalic
palaeohighs were documented and published separately in
to tholeiitic magmatism, steeply dipping bounding faults, our previous studies carried out at various localities
and low but long-term extension (Morley 1989; Leeder through the northern Turkey (Ko(cid:141)yi(cid:219)it 1987; Ko(cid:141)yi(cid:219)it &
1995). In contrast, supradetachment basins develop over Alt(cid:221)ner 1990; Ko(cid:141)yi(cid:219)it et al. 1991a, b; Alt(cid:221)ner et al.
young orogens and/or back-arc settings, and occur in 1991). In order to avoid repetition of details of the local
highly extended terrains such as the United States data, only the simplified pattern of measured
Cordillera, the Cyclades islands in the northern Aegean stratigraphical sections (1—14 in Figure 1) will be used in
Sea, and the present-day Western Anatolian region in the present paper. For detailed information the readers
Turkey. Therefore, they are associated with thick or are referred to the afore-mentioned papers. One
overthickened, hot and young crust, and are exception to this is the (cid:220)nek(cid:154)y study that includes new
characterized by tholeiitic to calc-alkalic magmatism, high findings on Jurassic volcanic rocks of the Ankara region.
but relatively short-term extension and low-angle For this reason, a detailed stratigraphic section of the
bounding faults (Friedmann & Burbank 1995). (cid:220)nek(cid:154)y (Ankara) area will also be given here.
One well-preserved example of a supradetachment
basin is the Jurassic—Early Cretaceous north Anatolian Summary of Late Palaeozoic—Early Mesozoic
palaeorift (NAPR). It is exposed as discontinuous inliers of
Palaeogeographic Evolution and Tectonic Setting of
varying size within, and to the north of the Late
the NAPR
Cretaceous—Early Tertiary (cid:220)zmir-Ankara-Erzincan suture
Although views on Palaeo-Tethys, Neo-Tethys and their
((cid:220)AEZ), throughout northern Turkey (Figure 1A). The
NAPR comprises the northern passive continental margin subduction directions remain controversial, all of these
170
A. KO(cid:130)Y(cid:220)(cid:218)(cid:220)T & D. ALTINER
gd
nn
NNN000100100100kmkmkmBLACK SEABLACK SEABLACK SEA PlatformPlatformPlatform141414TroughTroughTrough7YYYusufeliusufeliusufeli9SEA OFSEA OFSEA OF4313MARMARAMARMARAMARMARA?10AAA11EEE82SSS???6 12NNN(cid:221)(cid:221)(cid:221)AAA15AAAEEEEEESSSGGGANKARAANKARAANKARAAAAEEEHal(cid:253)larHal(cid:253)larHal(cid:253)larAAA H-TH-TH-T: Hettangian-Toarcian: Hettangian-Toarcian: Hettangian-ToarcianTr : TriassicOxf-Apt: Oxfordian-AptianC-Br: Callovian-BerriasianC-Br: Callovian-BerriasianC-Br: Callovian-Berriasianbasal conglomerate of Malm ageH-Plb: Hettangian-PliensbachianH-Plb: Hettangian-PliensbachianH-Plb: Hettangian-PliensbachianAU: angular unconformityOxf-Bar: Oxfordian-BarremianOxf-Bar: Oxfordian-BarremianOxf-Bar: Oxfordian-BarremianBaj-Br: Bajocian-BerriasianBaj-Br: Bajocian-BerriasianBaj-Br: Bajocian-Berriasianpelagic cherty carbonateH-Bt: Hettangian-BathonianH-Bt: Hettangian-BathonianH-Bt: Hettangian-BathonianD: disconformity-paraconformityD: disconformity-paraconformityD: disconformity-paraconformityOxf-VOxf-VOxf-V: Oxfordian-Valanginian: Oxfordian-Valanginian: Oxfordian-ValanginianBaj-VBaj-VBaj-V: Bajocian-Valanginian: Bajocian-Valanginian: Bajocian-ValanginianN-R: Norian-RhaetianN-R: Norian-RhaetianN-R: Norian-RhaetianN: nonconformityN: nonconformityN: nonconformityC-Apt: Callovian-AptianC-Apt: Callovian-AptianC-Apt: Callovian-Aptianshallow-water platform carbonateBt: Bathonian (proto-rift unconformity) (proto-rift unconformity) (proto-rift unconformity)Plb-Bt : Pliensbachian-BathonianC-Ht: Callovian-HauterivianC-Ht: Callovian-HauterivianC-Ht: Callovian-HauterivianH-Apt: Hettangian-AptianH-Apt: Hettangian-AptianH-Apt: Hettangian-Aptianpelagic to turbiditic cherty carbonates with slopebreccia, olistostromes and slump folds alternation of tuff, tuffite, pillow basalt, olistostrome,pelagic oolitic cherty carbonate intruded by diabase sill4.4.4.AKTA(cid:222)AKTA(cid:222)AKTA(cid:222) (GEREDE)(GEREDE)(GEREDE)alternation of tuffite, tuff, pelagic carbonate, and turbiditeSantonianSantonianSantonianmedium- to fine-grained clastics with coal seams12.12.12.AKDA—AKDA—AKDA— DDD6.HASANO—LAN(ERZ(cid:221)NCAN)(ERZ(cid:221)NCAN)(ERZ(cid:221)NCAN) 10.10.10.continental to shallow marine clastics with AmmoniticoBERD(cid:221)GABERD(cid:221)GABERD(cid:221)GA (ANKARA)Rosso facies((cid:222)EB(cid:221)NKARAH(cid:221)SAR)((cid:222)EB(cid:221)NKARAH(cid:221)SAR)((cid:222)EB(cid:221)NKARAH(cid:221)SAR)3.3.3.MUDURNUMUDURNUMUDURNU 9.9.9.RE(cid:222)AD(cid:221)YERE(cid:222)AD(cid:221)YERE(cid:222)AD(cid:221)YETTTuronianuronianuronian(BOLU)(BOLU)(BOLU) Lower-Middle Liassic volcaniclastic rocks with pillow13.13.13.(TOKAT)(TOKAT)(TOKAT)BABABAYBURTYBURTYBURTDDDbasalts, diabase sills and Ammonitico Rosso intercalations1. 1. 1111. KELK(cid:221)TKELK(cid:221)TKELK(cid:221)TPalaeocenePalaeocenePalaeocene(ERZ(cid:221)NCAN)(ERZ(cid:221)NCAN)(ERZ(cid:221)NCAN)14. 14. 14. YUSUFEL(cid:221)YUSUFEL(cid:221)YUSUFEL(cid:221)777LAD(cid:221)KLAD(cid:221)KLAD(cid:221)K5.Hettangian-Pliensbachian Ammonitico Rosso faciesHettangian-Pliensbachian Ammonitico Rosso facies. . . DDDConiacianConiacianConiacian(cid:221)NEK(cid:214)Y8.8.8. KUMLUCAKUMLUCAKUMLUCA(ARTV(cid:221)N)(ARTV(cid:221)N)(ARTV(cid:221)N) (SAMSUN)(SAMSUN)(SAMSUN)(ANKARA)(TOKAT)(TOKAT)(TOKAT)TTTuronianuronianuronianLower Liassic basal conglomerateDDDttt2. 2. 2. pppG(cid:220)NYG(cid:220)NYG(cid:220)NYARIKARIKARIKVVVrrrtttAAADBBBCampanianCampanianCampanianppptttrrr---DDDppp1.1.1.(BOZ(cid:220)Y(cid:220)K)(BOZ(cid:220)Y(cid:220)K)(BOZ(cid:220)Y(cid:220)K)aaajjjAAA---HALILARHALILARHALILARAalenian-Bathonian coarse----aaaAAABBB fffjjjVVVDDDBBB---aaaxxxDDD---VVV---CCC(EDREM(cid:221)T)(EDREM(cid:221)T)(EDREM(cid:221)T)grained sandstonesBBBrrrOOO---fffCCCBBBjjjxxxDDD---aaaDDDfffDDDOOODDD---tttBBBxxxHHHCCCDDDOOONorian-Toarcian fine clasticstttrrr---pppDDDBBBCCCDDDAAAbbbbbbDDD---tttlll---CCCTriassic KarakayatttBBBlllPPPHHHppprrrPPPbbb---BBB---bbbAAAD (?)---lllHHHTTTbbbrock assemblageHHHPPPlll---bbb---PPPlllCCC------lllbbbPPPHHHDDDHHH---PPPHHHTTTllllll???HHHPPPbbb---tttpre-Jurassic mafic to---???HHHNNNBBBHHHNNNPPPN---NNNNNN???NNNAUAUAUHHHNNN---NNNultramafic rocksm???HHHtttm BBB0rrr ---TTT00pre-Jurassic metavolcanic rocksmHHH30mmm 2m0 m00mmRRR 0mm pre-Permian metagranitoid0000 1---0 0 m 2 200NNN00m0011BBB000 020 pre-Permian polyphase65402008low-grade metamorphic rocks4 e 1.(A)Simplified map showing type localities (Numbers 1 through 14) of the North Anatolian Palaeorift infill. (cid:220)AES- (cid:220)zmir-Ankara-Erzincan Suture; (B)Stratigraphical sections showiboth the lateral and vertical facies distribution of the North Anatolian Palaeorift infill. Sections 7, 9, 10, 11, 13 and 14 were compiled in addition to authors own field studies ameasurements, from (cid:133)zt(cid:159)rk (1973), Seymen (1975), Rojay (1985), G(cid:159)rsoy (1989), Wedding (1963), and Baydar et al.(1967), respectively.
r
u
g
Fi
171
NORTHANATOLIAN PALAEORIFT
ideas can be categorized into two general groups: (1) Stratigraphic Outline
Those studies referring to Tethys as a single oceanic basin
Stratigraphical and sedimentological characteristics of the
system subducting northward in the eastern
NAPR infill were studied in detail by both geological
Mediterranean region that persisted at least from
mapping at a 1/25,000 scale and by stratigraphical
Permian until Early Tertiary times (Robertson & Dixon
sections measured at 14 type localities (Figure 1). The
1984; Robertson et al. 1991; Stampfli et al. 1991;
basement rocks are beyond the scope of this paper, and
Dercourt et al.1993; Usta(cid:154)mer & Robertson 1997; Okay
only brief information about them will be given below.
& T(cid:159)ys(cid:159)z 1999); (2) According to other groups of
studies, there was a super oceanic basin system composed
of a southward subducting Palaeo-Tethys of Basement Rocks
Carboniferous-Mid Jurassic age and a northward At locations 3, 4, 9 and 10 in Figure 1, the basement of
subducting Neo-Tethys of Triassic-Early Tertiary age the north Anatolian palaeorift is not observed. In
((cid:222)eng(cid:154)r 1979; (cid:222)eng(cid:154)r & Y(cid:221)lmaz 1981; Ko(cid:141)yi(cid:219)it 1987, contrast, at the remaining type localities, the basement
1991a; Ko(cid:141)yi(cid:219)it et al.1991a; Y(cid:221)lmaz et al.1997). Our consists of one or more of the following rocks of the
recent field, stratigraphical, palaeontological and Palaeo-Tethyan orogen: (a) pre-Permian (?) polyphase
sedimentological data, which will be presented in detail low-grade metamorphic rocks, (b) pre-Permian
below, support the second general view. metagranitoid, (c) pre-Jurassic metavolcanic rocks, (d)
pre-Jurassic ultramafic rocks to mafic rocks, and (e) the
During the Carboniferous—Permian interval, the
Triassic Karakaya palaeorift fill (Figure 1B).
northern part of present-day Turkey (Pontides), with the
exception of the (cid:220)stanbul-Zonguldak Zone and the (a) The first group of widespread basement rocks
Hercynian basement of the future Sakarya Continent, comprises polyphase low-grade metamorphic rocks. They
constituted the northern convergent margin of consist mainly of green schists, marble, metavolcanic
Gondwanaland (Robertson & Dixon 1984; (cid:222)eng(cid:154)r et al. rocks, metamafic to ultramafic rocks, and rarely higher-
1984; Y(cid:221)lmaz et al.1997; Alt(cid:221)ner et al.2000). However, grade metamorphic rocks such as gneiss, amphibolite and
during the Early and Mid-Triassic, the Hercynian glaucophane schist. They are well observed at locations 5,
basement of the future Sakarya Continent included a 7, 8, 12 and 14 in Figure 1. Their age is still controversial
magmatic arc situated on the southerly subducting ocean (Okay 1983; Ko(cid:141)yi(cid:219)it et al. 1991b; Gen(cid:141) & Y(cid:221)lmaz
floor of Palaeo-Tethys and became the site of 1995).
sedimentation for the Karakaya marginal basin ((cid:222)eng(cid:154)r (b) The Hercynian granitoids are widely exposed in
1979; (cid:222)eng(cid:154)r & Y(cid:221)lmaz 1981; Y(cid:221)lmaz et al. 1997). the west and east of northern Turkey as shown in
During the Late Triassic, the Karakaya rock assemblage locations 2, 11, 13 and 14 in Figure 1. They are
and its Hercynian basement were intensely deformed and represented mainly by metagranite, leucogranite and
became the northern part of Gondwanaland owing to the granodiorite cut by aplite and microdiorite dikes. In
closure of the Karakaya marginal basin (Figure 2A). In places, the granitoids intruded the low-grade
Hettangian time, a new rifting process began within this metamorphic rocks. According to disputable radiometric
very young and flexurally to isostatically-uplifted orogen dating carried out by (cid:130)o(cid:219)ulu (1975) and Bergougnan
(Figure 2B,C) (G(cid:154)r(cid:159)r et al.1983; Ko(cid:141)yi(cid:219)it 1991a; Alt(cid:221)ner (1987), their ages may range from 280 My to 360–2 My
et al.1991; Ko(cid:141)yi(cid:219)it et al. 1991a; Y(cid:221)lmaz et al.1997). (Carboniferous).
This new rifting (Figure 2D) triggered the development
(c) The pre-Jurassic metavolcanic rocks are exposed
of both the NAPR and northern Neo-Tethys ((cid:220)zmir-
only in location 8 (Figure 1). They are mostly andesitic in
Ankara-Erzincan Ocean). The former is here interpreted
composition.
as a large and composite supradetachment basin
(d) The fourth basement rock suite is composed of
constituting the northern passive continental margin of
pre-Jurassic ultramafics and mafic rocks. They are
Northern Neo-Tethys in Jurassic—Early Cretaceous times
observed at location 12 (Figure 1) where they are in
(Figure 2E).
thrust-fault contact with low-grade metamorphic
basement. These rocks occur as tectonic slabs or sheets
172
A. KO(cid:130)Y(cid:220)(cid:218)(cid:220)T & D. ALTINER
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D BLOCK FAULTING AND ONSET
(HETTANGIAN-APTIAN) OF SYN-RIFT SEDIMENTATION
HALILAR-BURSAHALILAR-BURSAHALILAR-BURSA B(cid:221)LEC(cid:221)K PLAB(cid:221)LEC(cid:221)K PLAB(cid:221)LEC(cid:221)K PLATFORMTFORMTFORM DROWNED PLADROWNED PLADROWNED PLATFORMTFORMTFORM(SUBPLATFORM)(SUBPLATFORM)(SUBPLATFORM) BBBAAA(((SSSiiinnnMMMIIItttNNNeeeUUUrrrAAAiiiDDDoooLLLrrrUUU TTTgggRRRrrrRRRaaaNNNOOObbbUUUeeeUUUnnnGGG)))HHH AKTAKTAKTA(cid:222)-INEKOYA(cid:222)-INEKOYA(cid:222)-INEKOY PPPALAEOHIGHALAEOHIGHALAEOHIGH(Platform)(Platform)(Platform) DROWNEDDROWNEDDROWNEDPLAPLAPLATFORMTFORMTFORM(subplatform)(subplatform)(subplatform) BBBAAA(((SSSiiinnnKKKIIItttNNNeeeUUUrrrAAAiiiMMMoooLLLrrrLLL TTTgggUUUrrrRRRaaaCCCOOObbbAAAeeeUUUnnnGGG)))HHHDROWNED PLADROWNED PLADROWNED PLATFORMTFORMTFORM(subplatform)(subplatform)(subplatform) BERD(cid:221)GA-KELK(cid:221)TBERD(cid:221)GA-KELK(cid:221)TBERD(cid:221)GA-KELK(cid:221)TPPPALAEOHIGHALAEOHIGHALAEOHIGHBBBAAA(Platform)(Platform)(Platform)SSSIIINNNAAAAAAKKKLLLDDD TTTAAARRR———OOOUUUGGGHHHBABABAYBURT-YUSUFELI(cid:221)YBURT-YUSUFELI(cid:221)YBURT-YUSUFELI(cid:221)PALAEOHIGHPALAEOHIGHPALAEOHIGH(Platform)(Platform)(Platform)
(((iiinnnttteeerrriiiooorrr gggrrraaabbbeeennn)))
111 VVVAAAGGG 222HHHBBBGGG 333 444 555VVVCCCGGG 666---777 888 999 111000---111111 111222 111333VVV---CCC111444eeeGGG
HHHCCCeeeGGG
MFC PPPTTTRRRUUU
SSSRRRUUU
KKKRRRBBB PPPRRRUUU
kkk666mmm OOOMMMFFFSSS IIIMMMFFFSSS
E IIIMMMFFFSSS OOOMMMFFFSSS IIIMMMFFFSSS OOOMMMFFFSSS
basal association (see Figure 1 for distribution basinal association
of volcanic and volcaniclastic rocks and
Ammonitico Rosso facies) platform carbonates
Norian-Rhaetian shallow-marine finer clastics basal conglomerate
pre-Hettangian basement rocks lower condensed sequence (((nnnooottt tttooo
Figure 2. (A)Plate tectonic framework showing the future site of North Anatolian palaeorift. SL: sea level; (B)uplift and
subvertical fracturing; (C) formation of proto-rift unconformity; (D)block faulting and initial sedimentation of
the North Anatolian Palaeorift infill, and (E) diagrammatic three-stage graben model depicting the fully
developed North Anatolian Palaeorift. HBG- Hauterivian—Barremian gap, HCeG- Hauterivian—Cenomanian gap,
IMFS- inner master fault system, KRB- Karakaya remnant basin, MFC- marginal fault complex, OMFS- outer
master fault system, PRU- pre-rift unconformity, PTRU- post-rift unconformity, SRU- syn-rift unconformity,
VAG- Valanginian-Aptian gap, VCG- Valanginian-Coniacian gap, and VCeG- Valanginian-Cenomanian gap.
173
NORTHANATOLIAN PALAEORIFT
of varying size, and consist mainly of serpentinized, conglomerate on the erosional surface of the afore-
sheared and brecciated peridotite, harzburgite, mentioned basement rocks with angular unconformity or
hornblende gabbro, diorite and diabase with minor nonconformity (Figure 1). It is an unsorted to poorly
amounts of basalts (Ko(cid:141)yi(cid:219)it 1991a). sorted polygenetic fan conglomerate and consists of well
rounded to sub-angular pebbles and cobbles ranging from
(e) The fifth basement rock is a tripartite facies
a few cm to 1.5 m in diameter. The clasts comprise
association characterizing the Triassic Karakaya rift. It is
granite, quartz, marble, Permian to Triassic recrystallized
well exposed at locations 6 and 7 in Figure 1 and consists,
limestone, schist, phyllite, spilitic basalt, serpentinite,
from bottom to top, of arkosic clastics, alternations of
metaultramafic rock, chert and radiolarite. These clasts
shallow-marine carbonate, pillow basalts and their
are set in a litharenitic matrix bounded by a ferruginous
pyroclastic equivalents, and a wildflysch. Based on fossil
and siliceous to limy cement.
content, this association is considered to be Triassic in age
(Ko(cid:141)yi(cid:219)it et al.1991b; Alt(cid:221)ner & Ko(cid:141)yi(cid:219)it 1993). The basal conglomerate is mostly massive or very
thick-bedded. It occasionally displays some sedimentary
Finally, in the Hal(cid:221)lar area only (location 1 in Figure
structures such as cross-bedding, pebble imbrication,
1), the North Anatolian palaeorift fill has a transitional
graded bedding and mesoscopic growth faults. This
contact relationship with underlying Triassic fine-grained
conglomerate also contains sandstone lenses and plant
clastics of the remnant Triassic Karakaya rift (Ko(cid:141)yi(cid:219)it
fragments and ranges in thickness from a few meters up
1990).
to 200 m. Although no diagnostic marine or continental
fossils have been found within the basal conglomerate, it
North Anatolian Palaeorift Infill is followed by shallow-marine clastics or a Ammonitico
Rosso facies of late Hettangian—Pliensbachian age
On the basis of depositional settings and facies, the NAPR
(Ko(cid:141)yi(cid:219)it 1987; Alt(cid:221)ner et al.1991; Nicosia et al.1991).
infill is divided into three basic facies associations: basal
It is interpreted as a continental-fan conglomerate
association, platform association, and basinal association
deposited by debris flow and braided-river systems.
(3, 4, 6 and 7 in Figure 2E). The basal facies association
constitutes the syn-rift infill, whereas both the platform
and basinal associations represent the post-rift infill.
Continental to Shallow-marine Clastics—These rocks are
well exposed in the Bilecik area (Alt(cid:221)ner et al.1991) and
at type localities 1, 5, 6 and 12 (Figure 1). They start
The Basal Association—Except for the Hal(cid:221)lar area (1 in
with a coarse-grained arkosic sandstone on an erosional
Figure 1), the basal association rests unconformably on
surface of the basement rocks, or conformably follow the
an erosional surface of the pre-Hettangian basement
basal conglomerate. They comprise alternations of
rocks. In contrast, at the top, it passes into the basinal
medium- to thick-bedded shallow-marine sandstone, thin-
association at locations 3, 8 and 12, while it is overlain
bedded to laminated, green-yellow siltstone, shale, marl,
unconformably by platform carbonates at the remaining
turbiditic sandstone and red mudstone to marl with
locations (Figure 1).
volcanogenic sandstone intercalations; the latter unit is
The basal association ranges from 100 m to 3.8 km
possibly the first product of rift volcanism in the NAPR.
in total thickness, and consists mainly of five basic units
These alternations contain lenses of both calcareous and
of varying thickness that have both lateral and vertical
marly Ammonitico Rosso facies, with rich associations of
transitional contact relationships. These are: (1) basal
ammonites (Alkaya 1979; Cope 1991), brachiopods
conglomerate, (2) continental to shallow-marine clastics
(Ager 1991), bivalves and gastropods (Conti & Monari
with intercalation of volcaniclastic rocks, (3) Ammonitico
1991) belemnites (Doyle & Mariotti 1991), crinoids
Rosso deposits, (4) volcaniclastic and volcanic rocks, and
(Nicosia 1991) and foraminifera (Alt(cid:221)ner 1991; Alt(cid:221)ner et
(5) coal- and gypsum-bearing clastic rocks.
al.1991); this fauna constrains the age of these shallow
marine rocks as Hettangian—Pliensbachian (Ko(cid:141)yi(cid:219)it
1987; Alt(cid:221)ner et al. 1991; Nicosia et al. 1991). The
Basal Conglomerate—At the type (2, 5, 6, 7, 8, 11, 12,
continental to shallow-marine clastics range in thickness
13, 14) localities, the NAPR fill starts with a basal
from 100 m to 700 m.
174
A. KO(cid:130)Y(cid:220)(cid:218)(cid:220)T & D. ALTINER
Ammonitico Rosso Deposits— These deposits occur as continental basal conglomerate or coarse-grained arkosic
lenses, a few metres to 250 m long, 30 cm to 70 m in sandstone. They consist of alternations of volcanogenic
thickness, or as 1-cm to 10-cm-thick beds alternating sandstone, tuffite, tuff, volcanic breccia, spilitic pillow
with shallow-marine fine-grained clastic rocks. basalt, andesitic lava, shale, mudstone, turbiditic
Ammonitico Rosso deposits are of three major types: (a) sandstone and pelagic carbonate. They also contain coal
nodular calcareous Ammonitico Rosso, (b) clayey-nodular seams, Ammonitico Rosso lenses, petrified wood and
marly Ammonitico Rosso, and (c) red silty Ammonitico plant-debris intercalations, and are intruded by diabase
Rosso. The nodular calcareous Ammonitico Rosso also sills. The total thickness ranges from 50 to 3000 m
occurs in three sub-facies which are the stromatolitic (Wedding 1963; Nebert 1964; Alp 1972; Seymen 1975;
nodular limestone, bioturbated and bioeroded limestone Pelin 1977; (cid:133)zt(cid:159)rk 1979; Ketin 1983; G(cid:159)rsoy 1989;
and true nodular limestone. The nodular calcareous Saner 1990; Ko(cid:141)yi(cid:219)it et al.1991a, b).
Ammonitico Rosso facies is massive to thick-bedded and
The volcaniclastic and volcanic rocks have a
grey to pinkish in colour. It shows a transitional bottom
transitional contact with underlying continental basal
contact relationship with the underlying coarse-grained
conglomerates and arkosic sandstones. At the top, they
and shallow-marine sandstones, but a sharp to faulted-
either pass upward into the basinal pelagic association, as
contact relationship with the overlying relatively deep-
in the Mudurnu and Kumluca areas (3, 4 in Figure 1), or
marine and fine-grained turbiditic clastic rocks. It is
they are overlain disconformably by platformal
composed of oobiosparite to oobiomicrite and includes
successions ranging from coal-bearing clastics to shallow-
karstic features and cracks with iron-rich infill; it lacks
marine carbonates (2, 5, 7, 9, 10, 11, 13, 14 in Figure
evidence of terrigenous influx. All of these characteristics
1). Based on both their stratigraphical position and the
indicate deposition on a shallow plateau or seamount
Ammonitico Rosso deposits included in the volcaniclastic
open to the influence of wave action (Bernouilli & Jenkyns
and volcanic rocks, their age ranges from Pliensbachian
1974; Nicosia et al.1991).
(or pre-Pliensbachian in the Liassic) to Callovian. For
On the other hand, the clayey-marly and silty example, in the Mudurnu and Akta(cid:223) areas (3, 4 in Figure
Ammonitico Rosso deposits occur as lensoidal 1), volcaniclastic and volcanic rocks are overlain
intercalations within relatively deeper-marine, fine- conformably by Callovian pelagic carbonates. In contrast,
grained clastics to turbidites which are rich in terrigenous in the G(cid:159)nyar(cid:221)k area (2 in Figure 1), the same
influx. The Ammonitico Rosso has transitional contact volcaniclastics are underlain conformably by the
relationships with fine-grained marine clastic rocks, and Hettangian—Pliensbachian Ammonitico Rosso deposits,
lateral discontinuity with high terrigenous content is but overlain disconformably by the Callovian shallow-
attributable to the influence of currents in relatively marine platform carbonates. Similar kinds of
deeper marine settings (Bernouilli & Jenkyns 1974; stratigraphical contact relationships are also observed in
Nicosia et al.1991). the Ladik, Kumluca and Re(cid:223)adiye areas (7, 8, 9 in Figure
1). All of these observations indicate that the early
As is widely observed throughout the Alpine belt,
volcanism began during the Pliensbachian or pre-
Ammonitico Rosso deposits are a key horizon within the
Pliensbachian stages of the Liassic and continued up into
Liassic basal units across northern Turkey. Based on
Callovian within basinal areas, such as the Mudurnu and
various fossil assemblages, a Hettangian—Pliensbachian
Kumluca troughs (3, 8 in Figure 1).
age is assigned to these deposits (Ko(cid:141)yi(cid:219)it 1987; Alt(cid:221)ner
et al.1991). Petrographical and petrochemical studies carried out
on these volcanic rocks by Bekta(cid:223) et al.(1987) indicate a
remarkable compositional polarity towards the south
Volcaniclastic and Volcanic Rocks—At the type localities 1,
from tholeiitic to calc-alkalic through to high-K calc-
6 and 12 (Figure 1), volcaniclastic and volcanic rocks are
alkalic to high-K calc-alkalic-alkalic. The polarity and
not observed. In contrast, except for the Mudurnu area (3
petrochemical characteristics of the volcanic rocks
in Figure 1), these rocks increase in amount and dominate
indicate a magmatic origin related to a southward
the basal association of the NAPR in an eastward direction
subducting Palaeo-Tethys oceanic crust ((cid:222)eng(cid:154)r et al.
(Figure 1). These rocks succeed the sedimentation of the
1980; Bekta(cid:223) et al.1987). This tholeiitic to calc-alkalic
175
NORTHANATOLIAN PALAEORIFT
magmatism is one of the distinctive characteristics of the Based on lithofacies and biofacies, the platform
rifting phase of a supradetachment basin situated on association is divided into two sequences: a lower
young orogens or in a back-arc setting (Friedmann & condensed sequence, and an upper platform carbonate
Burbank 1995). Consequently, the petrochemical sequence (see legend in Figure 1B).
characteristics of Pliensbachian—Callovian volcanic rocks
in Turkey support the supradetachment basin
Lower Condensed Sequence—The lowermost facies of the
interpretation of the NAPR.
condensed sequence changes with distance away from the
basinal trough. Near this trough it is a thin volcanic rock,
Coal- and Gypsum-bearing Clastics— A continental to or a maximum 1-m-thick basal conglomerate, but away
shallow-marine sequence occurs at locations 10, 11, 13 from the trough it comprises a 1-2-m-thick ammonite-
and 14 in the eastern part of northern Turkey (Figure 1). rich stromatolitic and pelletic condensed packstone. The
This sequence has a short-term erosional contact lower condensed sequence starts with one of these basal
relationship with underlying volcaniclastic to volcanic units and continues upward as 15-cm to 1-m-thick beds
rocks at locations 10, 11 and 13, and displays the same of strongly bioturbated, pinkish and iron-rich nodular
contact relationship with both underlying and overlying limestones. The nodular facies is usually composed of
units at location 14 (Baydar et al.1967). pelagic pellet- and oolite-rich packstones and rarely of
At locations 10, 11, 13, 14 (Figure 1), volcaniclastic grainstones. Pellets and oolites are bound by stromatolitic
and volcanic rocks are replaced upward by a sequence of algae resulting in the formation of bindstones or even
gypsum, green shale, marl and iron-rich, limy and cross- oncolitic packstones. The main part of the condensed
bedded sandstones that also includes 1-m-thick coal sequence is characterized by cherty dolomite and medium
seams. The total thickness of this sequence ranges from to thick-bedded, dark grey, siliceous limestones
40 m to 500 m. It passes upward into thick-bedded, composed of pelagic oolite and pelletic grainstones and
shallow-marine and oolitic platform carbonates with the packstones with abundant thin-shelled bivalves, and
exception of location 14, where it is overlain crinoid-rich pelletic and intraclastic packstones. In the
unconformably by a thick conglomerate (Figure 1). uppermost part, the condensed sequence becomes less
pelagic with the appearance of a Tubiphytesfacies, and is
Palynologic studies carried out on coal samples taken
from the Kelkit and Bayburt areas (11, 13 in Figure 1) replaced by the platform carbonates. The condensed
show that this sequence is Bajocian—Bathonian in age sequence ranges from 3 to 350 m in thickness and, based
(A(cid:219)ral(cid:221) et al.1965, 1966). on a very rich macro- and microfaunal-association, its age
ranges from Bajocian to early Kimmeridgian (Alt(cid:221)ner
1991; Alt(cid:221)ner et al.1991).
The Platform Association
Stromatolites, pelagic-fossil content (ammonites,
In general, the platform association is characterized by
Globochaete, Globuligerina), and condensed nodular
shallow-marine carbonates. It either rests unconformably
limestones with pelagic oolites and pellets indicate an
on an erosional surface of the underlying basal association
open marine but shallow-water depositional setting, such
(2, 5, 6, 7, 9 and 14 in Figure 1) or shows a transitional
as a seamount or pelagic continental plateau, during
contact relationship with it (1, 4, 10, 11 and 13 in Figure
sedimentation of the lower condensed sequence
1). In the same way, its upper contact is either
(Bernouilli & Jenkyns 1974; Jenkyns 1986) where
unconformable or transitional with the pelagic basinal
oolites formed under strong wave action.
association (Figure 1). Apart from these localities, the
outcrops of the platform carbonates also occur in the
Sivrihisar-Polatl(cid:221)-Haymana region underlying the fore-arc Upper Platform Carbonates—These carbonate rocks are
sequences of Cretaceous to Eocene age (Gautier 1984; conformable with the underlying condensed sequence but
Ko(cid:141)yi(cid:219)it & Alt(cid:221)ner in preparation). The age range of the display both transitional and erosional upper contact
platform association is from Bajocian in the Hal(cid:221)lar area relationships with the deep-marine pelagic levels of the
(1 in Figure 1) to Barremian in the Ladik area (7 in Figure basinal association. They range from 100 m to 1100 m
1), and its total thickness varies from 100 m to 1500 m. in thickness. Detailed palaeontologic studies on these
176
A. KO(cid:130)Y(cid:220)(cid:218)(cid:220)T & D. ALTINER
platform carbonates indicate an age range from Purser (1975). The regressive subsequence of the upper
Kimmeridgian to Aptian (Alt(cid:221)ner et al.1991). platform carbonates also displays a well-developed, short-
to long-term palaeohigh character. Starting from the
The upper platform carbonates occur in two major
Valanginian, the regressive subsequence begins to emerge
subsequences: (a) an upward-fining (transgressive)
and persists as a palaeohigh until succeeded by
subsequence, and (b) an upward-coarsening (regressive)
sedimentation of deep-marine facies of the basinal
subsequence. The upward-fining subsequence starts with
association on an erosional surface. Accordingly, near the
medium- to thick-bedded, beige to grey limestones.
uppermost contact of the regressive sequence, the blue-
These limestones consist of coral boundstones, bioclastic
green algal mudstones are cut by an erosional surface and
grainstones, oolitic, flat pebble- and pellet-rich
overlain disconformably by a pelagic facies of the basinal
packstones and grainstones, dasyclad algal and pelletoidal
association with ages varying from Aptian to Santonian.
wackestones, packstones and ostracod and pellet-rich
This erosional contact is marked by the occurrence of
packstones. Toward the top they pass, in turn, into thin-
karstic features, neptunian dykes consisting of a reddish
to medium-bedded cherty limestones and cherts and then
sediment rich in iron, silica and calcite indicative of short-
to radiolaria-bearing, thin-bedded to laminated
to long-term breaks in sedimentation. A
argillaceous pelagic carbonates. These upper levels
lithostratigraphical and biostratigraphical case study of
characterize the basinal association. In contrast, the
the well-developed palaeohigh of Akta(cid:223)-(cid:220)nek(cid:154)y (Figure 1)
regressive subsequence starts with limestones similar to
is described here.
the fining-upward sequence, but is followed by two
distinct horizons. The first horizon, forming the middle
part of the regressive subsequence, is characterized by
Akta(cid:223)-(cid:220)nek(cid:154)y Palaeohigh—Although the Akta(cid:223) and (cid:220)nek(cid:154)y
oncolite- and nerineid gastropod-rich grey-pinkish
sections (4 and 5 in Figure 1) represent different
limestones; these are rich in oncolitic, oolitic and pelletic
palaeogeographic domains within the Jurassic—Early
packstone, oncolitic grainstone to mudstone and
Cretaceous evolution of northern Anatolia, they are
bioturbated and pelletic mudstones. The second horizon,
conceptually gathered together in this study into an
which constitutes the upper part of the regressive
east—west-trending, two-dimensional graben model
subsequence, is characterized by beige to grey micritic
(Figure 2). The Akta(cid:223) succession was previously defined
and pelletic limestones containing requienid rudist
as one of the important sections representing the Akta(cid:223)-
accumulations at several levels. These latter limestones
Sekinindoruk high bordered from north, west and east by
are composed of various facies including bioturbated
the Mudurnu trough (Ko(cid:141)yi(cid:219)it 1987; Ko(cid:141)yi(cid:219)it et al.
mudstone, laminated, pelletic and birdseye mudstone and
1991a). The (cid:220)nek(cid:154)y section is possibly located on a more
oncolitic grainstone, mudstone, requienid rudist- and
southerly margin of this basinal trough (Figure 1),
oncolite-rich wackestone. The uppermost part of the
representing a similar kind of palaeohigh. The (cid:220)nek(cid:154)y
regressive subsequence is dominated by meter-scale
outcrop occurs as an inlier surrounded by Tertiary
cycles consisting of stromatolitic and requienid rudist
sedimentary cover-rock assemblages divided into several
levels.
formations, approximately 35 km northwest of Ankara
The regressive subsequence evolves vertically into (Figure 3).
back-reef deposits characterized by oncolitic and
The succession in the (cid:220)nek(cid:154)y section (5 in Figure 1;
bioturbated nerineid grainstones and packstones rich in
Figure 4), overlies basement rocks of pre-Jurassic age
foraminifera and dasyclad algae deposited in an intertidal
(metamorphic rocks of the Pazaryeri structural complex)
to subtidal environment. The requienid rudist limestones
and is basically characterized by two main sedimentary
alternate with birdseye-rich pelletic levels forming meter-
rock assemblages, namely a basal association and a
scale cycles laid down in subtidal, intertidal and supratidal
platformal association, both displaying the characteristics
zones. Similar regressive successions have been
of the NAPR infill.
previously described by Colacicchi et al. (1975) from
Two formations have been distinguished in the basal
Italy. The cycles forming the uppermost part of the
association (Figures 3 and 4). The lower-lying Y(cid:221)lg(cid:221)n(cid:141)ay
regressive subsequence resemble the (cid:210)grainy beach cycle(cid:211)
Formation measures about 18 m in thickness and consists
deposits described from the Jurassic of the Paris basin by
177
NORTHANATOLIAN PALAEORIFT
L
5
1 0
1
15 18 45
43 50 NNN
m
0
20 48 50
2
4
0
7
36 40
Y 55
(cid:214)
K
E 3
N 5 3
(cid:221) 2
2
3 4
4
0
5 4
4
4
4
5
4
2
6 4
5 45 40 36
3
30 50 52 40 4 32 er.
4035 Y(cid:253)lg(cid:253)n(cid:231)ayRivLer 75 L 50Jb60 5848 17 Lower Cretaceous inli
—
c
si
s
Recent sedimentsdisconformity(cid:221)n(cid:246)n(cid:252)s(cid:253)rt(cid:253) Formation (Plio-Quaternary)angular UnconformityTuztepe Formation(late Langhian-Tortonian)Uzunkaya Formation(late Langhian-Tortonian)angular unconformityAkp(cid:253)nar Limestone (Lutetian)angular Unconformity K(cid:253)n(cid:253)k Formation (Palaeocene)angular unconformityG(cid:252)n(cid:246)ren Limestone(Kimmeridgian-Berriasian)Ta(cid:254)(cid:231)(cid:253)bay(cid:253)r(cid:253) Formation(Callovian-Oxfordian)disconformityBay(cid:253)rk(cid:246)y Limestone (Liassic) Y(cid:253)lg(cid:253)n(cid:231)ay Formation (Liassic)nonconformityPazarc(cid:253)k structural complex (pre-Permian) including carbonateblocks (L) line of measured section reverse fault strike and dip of bedding strike and dip of foliation Geological map of the (cid:220)nek(cid:154)y Jura
48 75 3.
e
r
u
g
Fi
178