ORIGINAL ARTICLE

Foraminiferal biostratigraphy and sequence stratigraphyacross the mid-Carboniferous boundary in the Central Taurides,Turkey

Ayse Atakul-Ozdemir • Demir Altıner •

Sevinc Ozkan-Altıner • Ismail Omer Yılmaz

Received: 9 July 2010 / Accepted: 28 December 2010

� Springer-Verlag 2011

Abstract The Aladag Unit is one of the main tectonic

units in the Tauride Belt, located in southern Turkey. It

includes a continuous Paleozoic carbonate sequence

encompassing the mid-Carboniferous boundary, with out-

crops being especially well exposed in the Hadim region.

The boundary succession lithology is mainly composed of

carbonates with intercalated quartz arenitic sandstone lay-

ers. Based on foraminifers, four biostratigraphic zones have

been defined in the interval from the Upper Serpukhovian

to the Lower Bashkirian. These zones are, in ascending

order: the Eostaffella ex gr. ikensis—E. postmosquensis

Zone (Zapaltyubinsky Horizon, Upper Serpukhovian); the

Plectostaffella jakhensis—P. bogdanovkensis Zone, and

the Millerella marblensis Zone (Bogdanovsky Horizon,

lower Bashkirian); and the Semistaffella sp. Zone

(Syuransky Horizon, lower Bashkirian). The mid-Carbon-

iferous boundary occurs between the Eostaffella ex gr.

ikensis—E. postmosquensis Zone and the Plectostaffella

jakhensis—P. bogdanovkensis Zone. Boundary beds are

characterized by eight, repeatedly occurring microfacies

types, namely: (1) coated crinoidal packstone; (2) coated

bioclastic grainstone; (3) oolitic grainstone; (4) oolitic

packstone-grainstone; (5) intraclastic grainstone; (6) mud-

stone-wackestone; (7) quartz-peloidal packstone; and 8)

quartz arenitic sandstone. Based on microfacies stacking

patterns, various types of shallowing-upward cycles have

been recognized. Depositional sequences and sequence

boundaries are correlatable with those described from

North America and Russia and Carboniferous global

sea-level curves. The duration of cycles has been estimated

as 100 ky, suggesting that cycle periodicities correspond to

the Milankovitch eccentricity band.

Keywords Mid-Carboniferous boundary � Foraminiferal

zones � Microfacies analysis � Meter-scale cyclicity �Central Taurides

Introduction

The Mississippian-Pennsylvanian (mid-Carboniferous)

boundary is defined by the evolutionary appearance of the

conodont Declinognathodus noduliferus, with certain

foraminiferal species being useful as auxiliary indices.

Although there are several studies on calcareous foramin-

ifers of the mid-Carboniferous GSSP at Arrow Canyon

(Lane et al. 1972, 1999; Lane and Manger 1985; Brenckle

et al. 1977, 1982, 1997a, b), this datum in Turkey is not

directly correlatable with the American stratotype because

of foraminiferal provincialism as discussed in Groves

(1988). It is, however, possible to compare and correlate

the Turkish foraminiferal associations with Paleotethyan

and Uralian counterparts, particularly those described and

illustrated from the Russian Platform, Urals, and the

Donets Basin. By definition, the mid-Carboniferous

boundary coincides with the Serpukhovian-Bashkirian

stadial boundary in Russia and also with the Chesterian-

Morrowan boundary in the United States (Einor et al.

1979). In the 1970s and 80s, the mid-Carboniferous

boundary was placed at the top of the Voznessensky

horizon of the Russian Platform and correlated with the

boundary between the Bogdanovsky and Syuransky hori-

zons of the Urals. In the Donets Basin, it was placed at the

base of the E1 limestone (Aisenverg et al. 1979; Einor et al.

A. Atakul-Ozdemir � D. Altıner (&) � S. Ozkan-Altıner �I. O. Yılmaz

Department of Geological Engineering, Middle East Technical

University, 06531 Ankara, Turkey

e-mail: demir@metu.edu.tr

123

Facies

DOI 10.1007/s10347-010-0260-y

1979; Rotai 1979; Semichatova et al. 1979). Several

important studies adopted this scheme (Lys et al. 1978;

Vachard 1980; Altıner 1981; Vdovenko et al. 1990;

Vachard and Beckary 1991). However, following the

Carboniferous Meeting held in 1995 (Kagarmanov and

Kossovaya 1997), the boundary in the former Soviet Union

was adjusted downward to the contact between Zapaltyu-

binsky and Voznessensky horizons of the Russian Plat-

form, the base of the Bogdanovsky horizon of Urals and the

base of the C1d2 Zone of the Donets Basin. This modifi-

cation in the Paleotethyan-Ural realm is the fundamental

chronostratigraphic scheme for the most recent studies

(Vachard and Maslo 1996; Groves et al. 1999; Kulagina

and Sinitsyna 1997, 2003; Brenckle and Milkina 2003).

The main objective of the present study is to identify the

mid-Carboniferous boundary using calcareous foraminifers

within the context of high-resolution sequence stratigraphy

at a well-exposed section in the Taurides. Shallow-water

carbonates in the Hadim area are composed of upward-

shallowing cycles revealed by microfacies studies. It is well

established on the basis of previous studies (Goldhammer

et al. 1987, 1990, 1993; Strasser 1988; Goldhammer and

Harris 1989; Elrick and Read 1991; Osleger and Read 1991;

Elrick 1996) and on recent studies of Paleozoic and

Mesozoic successions of Taurides in Turkey (Altıner et al.

1999; Unal et al. 2003; Yılmaz et al. 2004; Yılmaz and

Altıner 2006), that stacking patterns of sedimentary cycles

are useful for the detection of sea-level changes. The

genetic organization of strata recognized in this study

reveals sequences comparable to those described by Ross

and Ross (1987), Alekseev et al. (1996), Lane et al. (1999),

Izart et al. (2003), Davydov et al. (2004), and Haq and

Schutter (2008) for the Paleozoic.

Geologic setting and measured section

The study area is located in the Aladag Unit of Ozgul (1976,

1984) approximately 10 km southwest of the town of Hadim

in the Central Taurides (Fig. 1). The Aladag Unit, one of the

allochthons of the Central Tauride Belt, is composed of

shelf-type carbonates and clastic rocks of Late Devonian

through Late Cretaceous age. In the study area, Devonian—

Triassic carbonate deposits of the Aladag Unit are widely

exposed and the Upper Paleozoic succession, in particular, is

nearly complete. The Aladag Unit locally is thrusted over

the Bolkar Dagı Unit, one of the other important allochthons

of the Tauride Belt (Fig. 1). The Paleozoic succession starts

with the Golbogazı Formation of Devonian age, comprising

quartz arenitic sandstones, shales, sandy limestones, and

reefal limestones. The overlying Carboniferous Yarıcak

Formation consists of shales, siltstones, and thinly bedded

limestones of the Tournaisian Cityayla Member and quartz

arenitic sandstones and limestones of the overlying Mantar

Tepe Member of latest Tournaisian to Gzhelian age (Altıner

and Ozgul 2001; Kobayashi and Altıner 2008a, b). The

Permian Cekic Dagı Formation is subdivided into four

members whose lithologies are quartz arenitic sandstones

and limestones. The Keltas and Camalan members are car-

bonates of Asselian to Artinskian age (Altıner and Ozgul

2001; Kobayashi and Altıner 2008a). They are overlain by

quartz arenitic sandstones of the Kizilgeris Member of

possible Wordian age, which constitutes the base of a thick

Middle to Upper Permian succession. Carbonates of the

Yellice Member of Wordian (?) to Changhsingian age rep-

resent the upper part of the formation (Altıner and Ozgul

2001; Altıner et al. 2007), which is paraconformably over-

lain by the Triassic Gevne Formation (Altıner and Ozgul

2001; Unal et al. 2003; Groves et al. 2005; Payne et al.

2007). The studied stratigraphic section, consisting of a

25.64-m-thick succession, was measured in detail through

the mid-Carboniferous boundary beds of the Mantar Tepe

member of the Yarıcak Formation (Fig. 2). The section is

characterized by four main lithologic intervals: a, b, c, and d

(see member column in Fig. 3). The succession starts with

quartz arenitic sandstones at the base and continues upward

with peloidal grainstones rich in quartz grains intercalated

with quartz arenitic sandstones (a). It passes upward into

bioclastic and oolitic limestones containing abundant mi-

crofossils and ooids (b). The middle of this interval includes

a prominent dark lime mudstone facies (Fig. 3). Towards the

upper part of the section, oolitic grainstones with quartz

fragments and quartz arenitic sandstones become dominant

(c). This interval is overlain by oolitic and bioclastic

grainstones including another dark limestone unit in the

upper part (d, Fig. 3).

Biostratigraphy

The studied section is divided into four foraminiferal zones

(Figs. 4, 5, 6, 7, 8) corresponding in age to the Zapaltyu-

binsky, Bogdanovsky and Syuransky horizons in the Upper

Serpukhovian to lowest Bashkirian of the Urals scheme

(Table 1). The Eostaffella ex gr. ikensis—E. postmosqu-

ensis Zone corresponds to the Upper Serpukhovian (Zap-

altyubinsky Horizon). The overlying Plectostaffella

bogdanovkensis—P. jakhensis Zone, Millerella marblensis

Zone and Semistaffella sp. Zone are early Bashkirian in age

and correlate to the Bogdanovsky and Syuransky horizons

(Fig. 4).

Eostaffella ex gr. ikensis—E. postmosquensis Zone

This zone encompasses the lower and middle parts of the

measured section and consists of quartz arenitic

Facies

123

sandstones, an alternation of quartz peloidal grainstones

and quartz arenitic sandstones, and the overlying oolitic

and coated bioclastic grainstones and packstones (upper

part of lithological interval a and lower part of lithological

interval b in Figs. 3, 4; samples 56 to 28). The interval

between samples 64 and 57, below the Eostaffella ex gr.

ikensis-E. postmosquensis Zone, has not been zoned due to

the absence of characteristic taxa. However, the presence

of Globivalvulina sp. suggests that this part of the section

deposited in continuity with the Eostaffella ex gr. ikensis-

E. postmosquensis Zone corresponds to the Serpukhovian

and probably to the Protvinsky Horizon.

The zone is characterized by the overlapping ranges of

two taxa, Eostaffella ex gr. ikensis and E. postmosquensis

and the upper boundary is marked by the last appearance of

E. ex. gr. ikensis. According to Vachard and Maslo (1996),

the last appearance of Eostaffella ikensis, based on the data

given in Einor et al. (1979), nearly corresponds to the

Serpukhovian-Bashkirian boundary. Similarly, Vdovenko

et al. (1990) reported the stratigraphic range of this taxon

from the Russian Platform as ranging from the Upper

Visean to the Serpukhovian—Bashkirian boundary,

including the Zapaltyubinsky Horizon. The lower boundary

of this zone is marked by the first appearance of E. post-

mosquensis in this study. In earlier studies, Vdovenko et al.

(1990) and Vachard and Beckary (1991) reported the first

occurrence of E. postmosquensis in the Serpukhovian,

below the Zapaltyubinsky Horizon. However, in more

recent studies (Vachard and Maslo 1996; Maslo and

Vachard 1997; Krainer and Vachard 2002; Kulagina et al.

2009) the first occurrence of E. postmosquensis was

reported at the base of the Zapaltyubinsky Horizon.

Fig. 1 a Location of the study area in Turkey. The box in the figure

corresponds to (b); b Geographic location of the study area near the

town of Hadim. The box in the figure corresponds to (c); c Geologic

map of the study area (after Altıner and Ozgul 2001) and location of

the measured section (MS)

Facies

123

This zone is considered to be equivalent to the Zapal-

tyubinsky Horizon in the Russian Platform and Donets

Basin (Vachard and Maslo 1996; Shcherbakov 1997), to

the upper part of the E2 Zone in Western Europe

(Vdovenko et al. 1990; Shcherbakov 1997) and to the

Ustsarbaisky Horizon in Urals (Rui et al. 1996) (Table 1).

Plectostaffella bogdanovkensis—P. jakhensis Zone

This zone consists of oolitic grainstones, coated bioclastic

grainstones, and oolitic packstones (upper part of litholog-

ical interval b and lowermost part of lithological interval c in

Figs. 3, 4; samples 27 to 18). It is defined as the interval from

the last occurrence of Eostaffella ex gr. ikensis to the first

occurrence of Millerella marblensis. The most characteristic

features of this zone are the first occurrences of Plectostaf-

fella bogdanovkensis and P. jakhensis at or very close to the

lower boundary. According to Vdovenko et al. (1990) and

Vachard and Maslo (1996), Eostaffella ex gr. ikensis became

extinct close to the Serpukhovian-Bashkirian boundary.

Vachard and Maslo (1996), Groves et al. (1999), and

Kulagina and Sinitsyna (1997, 2003) stated that the

appearance of Plectostaffella bogdanovkensis is a good

marker the Serpukhovian-Bashkirian boundary. Although,

Groves (1988), Vachard and Beckary (1991), and Vachard

and Maslo (1996) reported the first occurrence of the P.

jakhensis in the Syuransky Horizon, this form was observed

lower in our section and used for the determination of the

lower boundary of the zone. Altıner and Savini (1995)

reported P. jakhensis in equivalents of the Syuransky

Horizon in the Amazonas and Solimoes Basins in northern

Brazil. However, there is an unconformity at the base of

Pennsylvanian in these basins where equivalents of the

Bogdanovsky Horizon are missing.

This zone is equivalent to the lower Voznesensky Hori-

zon in the Russian Platform and the Donets Basin (Vdo-

venko et al. 1990; Vachard and Maslo 1996), the lower

Homoceras Zone in Western Europe (Vdovenko et al. 1990;

Vachard and Maslo 1996; Shcherbakov 1997) and the lower

Bogdanovsky Horizon in the Urals (Groves et al. 1994;

Fig. 2 Close-up view of the measured section. Letters a, b, c, and d stand for the lithologic intervals within the Mantar Tepe Member of the

Yarıcak Formation

Facies

123

Vachard and Maslo 1996; Kulagina and Sinitsyna 1997;

Shcherbakov 1997) (Table 1).

Millerella marblensis Zone

The interval between samples 17 and 12 (Fig. 4) is assigned

to this zone and is made up of coated crinoidal packstones,

coated bioclastic, oolitic grainstones with quartz fragments,

and quartz arenitic sandstones (lithological interval c and

lowermost part of lithological interval d in Fig. 3). It is

identified as the interval from the appearance of Millerella

marblensis to the first occurrence of Semistaffella sp. Va-

chard and Maslo (1996) first recognized this zone in the

upper Bogdanovsky Horizon. The upper boundary of this

zone was defined by Vachard and Maslo (1996) and

Kulagina and Sinitsyna (1997, 2003) on the entry of

Semistaffella.

The Millerella marblensis Zone corresponds to the

upper Voznesensky Horizon of the Russian Platform

(Vdovenko et al. 1990; Vachard and Maslo 1996), the

upper Homoceras Zone in Western Europe (Vdovenko

et al. 1990; Vachard and Maslo 1996; Shcherbakov 1997)

and to the upper Bogdanovsky Horizon of the Urals

(Groves et al. 1994; Vachard and Maslo 1996; Kulagina

and Sinitsyna 1997; Shcherbakov 1997) (Table 1).

Semistaffella sp. Zone

This zone is composed of oolitic and coated bioclas-

tic grainstones, a packstone facies, and a particular

Fig. 3 Columnar stratigraphic

section showing position of

mid-Carboniferous boundary

(S Stage, H horizon,

F formation, M member,

SN sample no)

Facies

123

mudstone facies representing the uppermost part of the

section (lithological interval d in Figs. 3, 4; samples 11

to 01). The lower boundary of the zone is defined by the

first occurrence of Semistaffella sp. The upper boundary

is not identified in this study because the top of the

measured stratigraphic section is within this zone. In

Ukraine and Russia, the lower boundary of the

Syuransky Horizon is also marked by the first occurrence

of Semistaffella (Vachard and Maslo 1996; Kulagina and

Sinitsyna 2003).

The Semistaffella sp. Zone corresponds to the Krasno-

polyansky Horizon of the Russian Platform (Vachard

and Beckary 1991; Vachard and Maslo 1996; Shcherbakov

1997), the Feninsky Horizon in the Donets Basin

Fig. 4 Fossil distribution chart

Facies

123

(Vachard and Maslo 1996) and the Syuransky Horizon

in the Urals (Vachard and Maslo 1996; Kulagina and

Sinitsyna 1997; Shcherbakov 1997) (Table 1).

Mid-Carboniferous boundary

The mid-Carboniferous boundary separates the Mississip-

pian and Pennsylvanian subsystems and it has been cor-

related to the Serpukhovian—Bashkirian boundary in

Russia. The basal Pennsylvanian (and basal Bashkirian)

GSSP at Arrow Canyon, Nevada (USA), was selected to

coincide with the first occurrence of the conodont Decli-

nognathodus noduliferus (Baesemann and Lane 1985; Lane

et al. 1999; Gradstein et al. 2004). Beds below the

boundary contain a rich association of archaediscid fora-

minifers dominated by Eosigmoilina robertsoni and Bren-

ckelina rugosa. Although the importance of these two

archaediscids for recognizing the boundary has been

mentioned in several studies (Brenckle et al. 1982, 1997a,

b; Skipp et al. 1985; Vdovenko et al. 1990; Harris et al.

1997; Baesemann et al. 1998; Kulagina and Sinitsyna

2003; Kulagina et al. 2008), they are known to range

upward into the lower part of the Pennsylvanian (Brenckle

et al. 1997a, b). At our section, Brenckelina rugosa is

totally absent and we observed a single occurrence of

Eosigmoilina just below the mid-Carboniferous boundary.

According to Groves (1988), the first occurrence of

Globivalvulina bulloides is useful for identifying the mid-

Carboniferous boundary. However, in recent studies from

Eurasia and Arctic Alaska, this species was recorded below

the mid-Carboniferous boundary (Vdovenko et al. 1990;

Harris et al. 1997; Baesemann et al. 1998). In our section,

Globivalvulina bulloides is present close to the base of the

Upper Serpukhovian Zapaltyubinsky Horizon. In the Bol-

shoi Kizil section in the Urals, Kulagina and Sinitsyna

(2003) reported Globivalvulina bulloides from even older

beds of the Steshevian-Protvian Horizons of the Ser-

pukhovian. Brenckle and Milkina (2003) also reported

Globivalvulina bulloides from the Protvinsky Horizon of

the Serpukhovian of the Tengiz Platform, Kazahsktan.

Finally, in one of the most recent studies, Vachard et al.

(2006), by discussing the problems on the taxonomy of

Biseriamminoidea, stated clearly that Globivalvulina

bulloides appeared below the mid-Carboniferous boundary,

more precisely in the late early Serpukhovian or Protvin-

sky. Among fusulinoideans, the genus Millerella previ-

ously was accepted as an informal marker of the mid-

Carboniferous boundary both in the western and eastern

hemispheres. It is now known that the genus originated in

late Mississippian time (Rauser-Chernousova et al. 1996;

Brenckle et al. 1997a, b; Gradstein et al. 2004). In the

Amazonas and Solimoes Basins, in northern Brazil, the

genus Millerella appears at the base of Pennsylvanian

(Altıner and Savini 1995). However, there is a gap at this

boundary corresponding to the lowermost Morrowan

(=Bogdanovsky Horizon) and so this appearance is strati-

graphically perched.

Although some of the important foraminiferal markers,

such as Eosigmoilina, Brenckelina, Eostaffella postmosq-

uensis, Eostaffella chomatifera were reported from the

Upper Serpukhovian—Lower Bashkirian strata of Libya

(Massa and Vachard 1979; Vachard et al. 1993), Tunisia

(Lys 1985), Algeria (Sebbar and Lys 1989; Mamet et al.

1994; Sebbar and Mamet 1999; Sebbar et al. 2000), and

Morocco (Mamet et al. 1966; Vachard and Tahiri 1991;

Vachard and Berkhli 1992; Berkhli et al. 1993, 2001;

Cozar et al. 2008), the mid-Carboniferous boundary has not

been delineated by carrying out a bed-scale sampling in

North Africa.

In the Paleotethyan-Uralian Realm, the most useful

foraminifers for recognizing the mid-Carboniferous

boundary are Plectostaffella jakhensis and P. bogdanovk-

ensis. Although the genus Plectostaffella has been reported

from the Upper Serpukhovian of Urals and Tien-Shan

(Einor 1996; Kulagina and Sinitsyna 2003; Orlov-Lab-

kovsky 2005; Nikolaeva et al. 2009), these two species are

reliable markers of the base of Pennsylvanian in most

places in the eastern hemisphere.

In Turkey, the mid-Carboniferous boundary was first

mentioned in the study by Altıner (1981). He placed the

Serpukhovian-Bashkirian boundary within his interval 12,

which was defined by the first appearance of Eostaffella

postmosquensis in the Late Serpukhovian and the first

appearance of Pseudostaffella antiqua in the Early Bash-

kirian. Following Vdovenko et al. (1990) and Vachard and

Maslo (1996), Altıner and Ozgul (2001) placed the mid-

Carboniferous boundary at the boundary between the Eo-

staffella postmosquensis—Plectostaffella ex gr. bogda-

novkensis Zone and the Semistaffella—Plectostaffella

jakhensis Zone. In accordance with the recent boundary

revisions, this boundary should be lowered down into the

Eostaffella postmosquensis—Plectostaffella ex gr. bogda-

novkensis Zone of Altıner and Ozgul (2001) where these

authors noted the first appearance of Plectostaffella ex gr.

bogdanovkensis following the first appearance of Eostaf-

fella postmosquensis. The lower part of this zone with

E. postmosquensis and Eostaffella ex gr. ikensis is now

assignable to the upper Serpukhovian (Zapaltyubinsky) and

the overlying interval with P. ex gr. bogdanovkensis is

correlative with the lower Bashkirian (Bogdanovsky).

The mid-Carboniferous boundary has been recognized

herein by the appearances of P. bogdanovkensis and

P. jakhensis and the last occurrences of Eostaffella ex gr.

ikensis. The range of the latter species is reported else-

where to terminate just below the mid-Carboniferous

Facies

123

boundary (Vdovenko et al. 1990; Vachard and Maslo 1996;

Altıner and Ozgul 2001; Nikolaeva et al. 2001). The mid-

Carboniferous boundary is drawn locally at the base of the

sample 27, coincident with the boundary between the Eo-

staffella ex gr. ikensis—Eostaffella postmosquensis Zone

and the Plectostaffella bogdanovkensis—P. jakhensis Zone

(Fig. 4).

Microfacies analysis

On the basis of bioclastic components and sedimentologi-

cal features observed in thin-sections, eight different mi-

crofacies have been identified. These are coated crinoidal

packstone, coated bioclastic grainstone, oolitic grainstone,

oolitic packstone-grainstone, intraclastic grainstone, mud-

stone-wackestone, quartz-peloid grainstone, and quartz

arenitic sandstone. These facies are grouped into four

facies associations that are assignable to four distinct

depositional belts (peritidal flat, lagoon, oolitic shoal, and

open marine). Major microfacies types comparable with

standard microfacies types (SMF) of Flugel (2004) are

summarized in Table 2. The microfacies and correspond-

ing depositional environments are discussed below.

Coated crinoidal packstone

The coated crinoidal packstone microfacies exhibits mi-

critic envelops around crinoid fragments and bioclasts

(Fig. 9a, b). Other components are superficial ooids, pel-

loids, dark intraclasts, foraminifers, bioclasts, brachiopods,

and gastropods.

This facies probably was deposited in open-marine,

moderately agitated conditions just below the wave base

(Wilson 1975; Elrick and Read 1991; Della Porta et al.

2004). It is equivalent of FZ 5 (platform margin reef) and

compatible with SMF 11 of Flugel (2004).

Coated bioclastic grainstone

This microfacies is essentially composed of bioclasts with

micritic envelopes. The major bioclastic components are

foraminifers (such as eostaffellids, archaediscids, palaeo-

textulariids, unilocular, and irregularly coiled bilocular

forms), crinoids, gastropods, brachiopods, and echinoid

fragments (Fig. 9c, d). Additional grain types are dark in-

traclasts, peloids, and rare ooids. Interparticle pores are

occluded by sparry calcite.

This facies occurs in areas of constant wave action at or

above wave base (Flugel 2004). It forms extensive sheets

generally seaward of oolitic grainstone shoals and grades

down dip into coated crinoidal packstone (Al-Tawil and

Read 2003; Della Porta et al. 2004). The coated bioclastic

grainstone microfacies is regarded as equivalent to SMF 11

and it corresponds to FZ 5 and FZ 6 (platform margin reef

and sand shoal) of Flugel (2004).

Oolitic grainstone

This microfacies consists mainly of ooids cemented by

sparry calcite (Fig. 9e, f). A variety of grains serve as the

nuclei, including intraclasts, quartz grains and skeletal

fragments, especially foraminifers. The laminae of the ooid

cortices exhibit radial fibrous structures. Superficial ooids,

characterized by a single lamina around the nucleus, are

also present in this grainstone. This facies is subdivided

into two subfacies, namely oolitic grainstone with bio-

clasts, and oolitic grainstone with quartz sand. The first

subfacies is moderately sorted and includes mainly fora-

minifers and other bioclast fragments together with ooids.

The other common constituents are intraclasts, peloids,

fragmented crinoids, and echinoids. The latter subfacies is

characterized by abundant, well-sorted ooids and fine

quartz sand.

This facies was deposited under high-energy, shallow-

water environments in platform margin sand shoals and

platform interior to open-marine settings (Elrick and Read

1991; Flugel 2004; Ahmad et al. 2006; Betzler et al. 2006;

Cozar et al. 2006; Armella et al. 2007; Barnaby and Ward

2007; Palma et al. 2007; Wanas 2008). The oolitic grain-

stone microfacies is equivalent to the SMF 15 of Flugel

(2004) and corresponds to FZ 6 and FZ 7 (platform-margin

sand shoal and restricted open marine) of Wilson (1975)

and Flugel (2004).

Oolitic packstone-grainstone

Radial fibrous ooids are the major components of this

microfacies. The microfacies consists mainly of ooids with

subordinate fossils, intraclasts, and peloids. The nuclei are

composed of bioclast fragments and dark intraclasts

Fig. 5 a–e Eostaffella postmosquensis, X100, a: HB04-27, b: HB04-

53; c: HB04-08; d: HB04-51; e: HB04-41, f–i Eostaffella postmosq-uensis acutiformis, X100, f: HB04-21, g: HB04-09; h: HB04-08; i:HB04-26, j–r Eostaffella pseudostruvei, X100, j: HB04-07; k: HB04-

08; l: HB04-08; m: HB04-11; n: HB04-04; o: HB04-11; p: HB04-19;

q: HB04-14; r: HB04-19, s Millerella angusta, X100, s: HB04-08,

t–u Eostaffella postproikensis, X100, t: HB04-32; u: HB04-33; v–xEostaffella ex gr. ikensis, X60, v: HB04-48; w: HB04-50; x: HB04-

27; y–z Eostaffella tenebrosa, X60, HB04-31, aa–ab Eostaffellapinguis, X100, aa: HB04-05; ab: HB04-04, ac–ae Eostaffellinaparaprotvae, X100, ac: HB04-21; ad: HB04-14; ae: HB04-04, af–aiPlectostaffella bogdanovkensis, X100, af: HB04-07, ag: HB04-17;

ah: HB04-14; ai: HB04-09, aj–al Plectostaffella jakhensis, X100,

aj–ak: HB04-07; al: HB04-05, am–an Plectostaffella varvariensis,

X100, am: HB04-05; an: HB04-17, ao–at Semistaffella spp., X100,

ao–aq: HB04-10; ar–at: HB04-11

c

Facies

123

Facies

123

(Fig. 9g). The grains are bound by sparitic to microsparitic

calcite cement, in places with micrite.

The radial fibrous ooids and poorly washed micritic

matrix indicate that this facies might have formed under

moderate to high energy (Folk 1959; Dunham 1962;

Lehrmann et al. 2001; Flugel 2004; Rott and Qing 2005).

This facies was deposited landward of the oolitic sand

shoal and equates to FZ 6 and FZ 7 (platform-margin sand

shoal and restricted open-marine settings) of Flugel (2004).

Intraclastic grainstone

This lithofacies is characterized by intraclasts, peloids,

coated and micritized skeletal grains, and aggregate grains.

Aggregate grains are composite grains consisting of ooids

and bioclasts bounded together by organic film of algal

origin and dark intraclasts (Fig. 9h). The most common

skeletal grains are echinoid fragments and foraminifers,

such as palaeotextulariids, pseudoendothyrids, globivalvu-

linins, eostaffellids, and unilocular forms. The intergranu-

lar spaces are mainly filled with sparry calcite cement.

This microfacies occurs under moderate water energy

levels (Flugel 2004). The presence of aggregate grains

indicates that this facies type was deposited in a shallow

subtidal environment with restricted circulation (Flugel

1982; Pomoni-Papaioannou and Kostopoulou 2008). The

intraclastic grainstone facies is comparable to SMF 17

(aggregate grain grainstone) and FZ 7 to FZ 8 of Flugel

(2004).

Mudstone-Wackestone

The mudstone-wackestone lithofacies is characterized by

abundant lime mud. It is poorly fossiliferous to unfossil-

iferous and contains peloids (Fig. 10a, b).

Lack of fossils and presence of vugs in this internally

featureless microfacies indicate a low-energy, restricted

lagoonal environment behind the high-energy sand

shoals (Al-Tawil and Read 2003; Al-Tawil et al. 2003;

Amirshahkarami et al. 2007; Barnaby and Ward 2007;

Wanas 2008). This microfacies corresponds to the standard

microfacies SMF-23 (non-laminated homogenous micrite

and microsparite) and FZ 9 of Flugel (2004), typical of the

shallow subtidal zone of a restricted, quiet water (lagoon)

setting.

Quartz-peloidal grainstone

This microfacies is unfossiliferous and composed of well-

rounded and abraded peloids, fine subangular quartz grains,

whole and abraded ooids, and skeletal fragments (Table 2;

Fig. 10c, d).

The cross-bedded quartz-peloidal grainstone microfa-

cies is interpreted as an eolianite on the basis of criteria

presented by Dodd et al. (1993) and Hunter (1993). The

eolian quartz-peloidal grainstones differ significantly from

marine grainstones in their abundant subangular quartz

grains and pelloids, microscopic grading, rounded broken

ooids and lack of in situ fossils (Hunter 1993; Smith and

Read 1999; Dodd et al. 1993, 2001; Abegg and Handford

2001; Smith et al. 2001; Al-Tawil and Read 2003;

Al-Tawil et al. 2003).

Eolianites can occur within transgressive or regressive

parts of sequences or both (Carew and Mylroie 2001;

Smith et al. 2001; Frebourg et al. 2008). Smith et al. (2001)

stated that eolinates overlying subaerial exposure surfaces

are interpreted to be deposited during transgressions.

Within our studied section, the eolian quartz-peloidal

grainstone facies probably was deposited during trans-

gression. It is commonly capped by the quartz-arenitic

sandstone facies and occurs at the base of cycles generally

recognized at the bottom of the measured section. It is

equivalent to FZ 10 (peritidal zone) of Flugel (2004).

Quartz arenitic sandstone

This microfacies consists of very fine quartz sand to silt.

Fossils and other constituents are absent. It comprises more

than 95% quartz grains (Fig. 10e, f). A fine-grained sparry

calcite to micrite is present between grains.

Herringbone cross-bedding indicates that the quartz

arenitic sandstone facies was deposited in an intertidal or

possibly a foreshore environment (Elrick and Read 1991;

Khalifa 2005). This microfacies is generally deposited

during the regressive phase and records sea-level lowstands

(Fischer and Sarnthein 1988; Barnaby and Ward 2007).

Cycles at the bottom of the studied section are capped by

this facies. It corresponds to FZ 10 (peritidal zone) of

Flugel (2004).

Fig. 6 a–f Pseudoendothyra spp., a: HB04-45, X60; b–c: HB04-11,

X60; d: HB04-59, X60; e: HB04-08, X60; f: HB04-38, X80; g–hParaarchaediscus koktjubensis, X100, g: HB04-40; h: HB04-41, i–kParaarchaediscus ninae, X140, i: HB04-51; j: HB04-24; k: HB04-46,

l–m Paraarchaediscus stilus, X100, l: HB04-51; m: HB04-54,

n Eosigmolina sp., X140, HB04-29, o–p Archaediscus postmoelleri,X140, o: HB04-40; p: HB04-04, q Archaediscus moelleri, X80,

HB04-59, r Archaediscus ex gr. karreri, X80, HB04-46,

s–v Archaediscus longus, X140, s–t: HB04-04; u–v: HB04-05,

w–y Neoarchaediscus probatus, X140, w: HB04-27; x: HB04-29; y:

HB04-27, z–ab Neoarchaediscus subbaschkiricus, X140, z: HB04-

09; aa: HB04-21; ab: HB04-26, ac–ae Neoarchaediscus achimensis,

X100, ac: HB04-47; ad–ae: HB04-32, af–ag Neoarchaediscusparvus, X140, af: HB04-49; ag: HB04-63, ah–aj Asteroarchaediscusbaschkiricus, X140, ah: HB04-51; ai: HB04-52, aj: HB04-32, ak–amAsteroarchaediscus rugosus, X140, ak: HB04-33; al: HB04-54; am:

HB04-30

c

Facies

123

Facies

123

Depositional model and facies distributions

A depositional model (Fig. 11) has been constructed for the

Serpukhovian—Bashkirian boundary beds on the basis of

detailed microfacies analysis and the successive occurrence

of microfacies types in the section. According to this

model, four major depositional belts are envisaged, (1)

peritidal, (2) lagoonal, (3) oolitic shoal, and (4) open

marine. In the peritidal depositional belt, the most abundant

microfacies types are quartz arenitic sandstone and quartz-

peloid grainstone (Fig. 11). The quartz-peloidal grainstone

facies is interpreted as eolianite on the basis of abundant

quartz grains and other petrographic features observed in

thin-sections (Hunter 1993; Dodd et al. 1993, 2001; Abegg

and Handford 2001; Smith et al. 2001). Elrick and Read

(1991), Smith and Read (1999, 2001), Smith et al. (2001),

Al-Tawil and Read (2003), and Al-Tawil et al. (2003)

reported that the quartz-peloidal grainstone and quartz

arenitic sandstone facies types are deposited in tidally

influenced shallow-marine or foreshore environments.

The lagoonal belt is characterized by low-energy con-

ditions and deposition of mudstone-wackestone facies

(Fig. 11). The mudstone-wackestone facies is interpreted to

be of low-energy, lagoonal origin on its lack of fossils,

presence of vugs, and association with shallow-marine

deposits (Al-Tawil and Read 2003; Al-Tawil et al. 2003;

Amirshahkarami et al. 2007; Barnaby and Ward 2007;

Wanas 2008).

An oolitic shoal was the likely setting in which intra-

clastic grainstone, oolitic packstone-grainstone, oolitic

grainstone, and coated bioclastic grainstone facies accu-

mulated (Fig. 11). Studies performed by Elrick and Read

(1991), Al-Tawil and Read (2003), Della Porta et al. (2004),

Flugel (2004), Betzler et al. (2006), Cozar et al. (2006),

Armella et al. (2007), Barnaby and Ward (2007), Palma et al.

(2007) and Wanas (2008) indicated that these grainstone and

packstone-grainstone facies packages were deposited in a

high-energy environment above the wave base.

The coated crinoidal packstone was mainly deposited

basinward of the oolitic shoal at or around the wave base

(Elrick and Read 1991; Al-Tawil and Read 2003; Della

Porta et al. 2004). Although, open-marine mudstone-wa-

ckestone facies was not observed in the studied section, the

presence of the mud-rich coated crinoidal packstone facies

indicates that open-marine mudstones might be found in

close proximity to the oolitic shoal belt whose seaward

depositional limit is controlled by the wave base (Fig. 11).

Meter-scale shallowing-upward cycles

Shallow-marine carbonates are reliable indicators of sea-

level fluctuations because their lithologic properties reflect

water depth, energy, and faunal content (Goldhammer et al.

1990). Detailed microfacies analyses of carbonates allowed

us to recognize shallowing-upward cycles in the studied

succession. Different types of cycles, mainly peritidal-

subtidal in character, are observed in this study based on

the vertical succession of the defined microfacies types and

associated subenvironments. Six different types of meter-

scale cycles are defined and microfacies variations within

these cycle types are as follows:

Cycle type: A

This type of cycle is characterized by peritidal facies

associations with abundant quartz fragments (Fig. 12).

Quartz-peloid grainstones at the bottom are followed

upward by quartz arenitic sandstones indicating relative

sea-level fall.

Cycle type: B

This type is composed completely of intraclastic grainstone

facies and the grain size of clasts, lumps, and biological

elements show a marked coarsening at the cycle tops

(Fig. 12). The upward increase in grain size is interpreted

to indicate a decrease in the rate of sea-level rise.

Cycle type: C

Coated bioclastic grainstone microfacies occurs at the

bottom of this type of cycle and the succession continues

upward with oolitic packstone-grainstone and oolitic

grainstone facies. It is capped by intraclastic grainstones

(Fig. 12, C1). In some cycles, mudstone-wackestone facies

is observed at the top of the cycles (C2). Other variations

are the absence of packstone-grainstone and intraclastic

grainstone facies at the cycle tops (C3).

Cycle type: D

This type is characterized by the dominance of oolitic

grainstones and displays two variations in capping facies at

the top of the cycle. It starts with oolitic grainstones with

abundant bioclastic grains and grades upward into oolitic

packstone-grainstone microfacies. The cycle is capped by

Fig. 7 a–f Globivalvulina sp., X100, a–d: HB04-43; e: HB04-52; f:HB04-44, g–m Globivalvulina bulloides, X100, g: HB04-44; h:

HB04-54; i–j: HB04-51; k: HB04-16; l: HB04-05; m: HB04-50,

n Globivalvulina sp., X100, HB04-44, o–q Bradyina cribrostomata,

X40, o: HB04-41, p: HB04-30, q: HB04-41, r Bradyina sp., X40,

HB04-44, s–v Endothyra spp., X80, s: HB04-11; t: HB04-20,

u: HB04-16; v: HB04-39, w Mediocris breviscula, X100, HB04-44,

x–y Mediocris mediocris, X100, x: HB04-24; y: HB04-51, z–aaMillerella umblicata, X100, z: HB04-11; aa: HB04-08, ab–adMillerella marblensis, X100, ab, ad: HB04-11; ac: HB04-10

c

Facies

123

Facies

123

the intraclastic grainstone facies with abundant lumps,

indicating shallowing-upward condition (Fig. 12, D1). This

cycle is sometimes incomplete because of the absence of

intraclastic grainstone facies at the top (D2).

Cycle type: E

In this type, coated crinoidal packstone facies occurs at the

bottom of the cycle and continues upward with the coated

bioclastic grainstone facies. Oolitic grainstones lying at the

top of the cycle establish an upward-shallowing cycle

(Fig. 12).

Cycle type: F

Coated crinoidal packstone facies occurs at the bottom and

the upper half of the cycle is characterized by oolitic

grainstones with quartz fragments (Fig. 12, F1). This type

of cycle is sometimes capped by quartz arenitic sandstones,

indicating a shallowing trend leading to subaerial exposure

(F2).

Sequence stratigraphic interpretation

A sequence stratigraphic interpretation is put forward

based on the microfacies associations of shallowing-

upward cycles and landward—basinward shifts in diag-

nostic facies belts. Vertical stacking patterns of the meter-

scale cycles are used to define systems tracts, large-scale

sequences, and sea-level fluctuations (Goldhammer et al.

1990; Osleger and Read 1991; Amirshahkarami et al.

2007). The vertical evolution of microfacies and the

interaction of cycle types within the studied section allow

the identification of two depositional sequences and part of

a third sequence (Fig. 13). Because of the absence of

exposure surfaces and erosional boundaries in the section,

sequence boundaries were identified by abrupt facies

changes. The first and third sequence boundaries in the

section were placed above quartz arenitic sandstones. The

second sequence boundary was placed at the top of the

mudstone-wackestone facies underlying relatively deeper,

coated bioclastic grainstone facies (Fig. 13).

Each sequence comprises a package of transgressive and

highstand systems tracts. The first sequence is marked by

peritidal lagoonal and oolitic facies associations. The

transgressive systems tract of the first sequence is domi-

nantly composed of siliciclastic facies and the highstand

systems tract is dominantly carbonate. The transgressive

systems tract consists of quartz arenitic sandstones, quartz-

peloidal grainstones, and intraclastic grainstone facies and

is characterized mainly by A and B-type cycles (Fig. 13).

In this sequence, the maximum flooding surface has been

placed at the base of coated bioclastic grainstone facies

(Fig. 13). The highstand systems tract consists of oolitic

shoal grainstones and lagoonal mudstone-wackestone

facies and comprises the genetical stacking of C1, C2, C3,

and D1, D2-type cycles (Fig. 13).

The second depositional sequence has been identified by

the deposition of relatively deeper, coated bioclastic

grainstones over lagoonal mudstone-wackestone facies.

The transgressive systems tract of this sequence is repre-

sented by C1 and D1 type cycles (Fig. 13) comprising

oolitic shoal facies, oolitic grainstones, coated bioclastic

grainstones, and intraclastic grainstones. The maximum

flooding surface is situated on top of the intraclastic

grainstones and at the base of the coated crinoidal pack-

stone facies. The highstand systems tract of this sequence is

represented by E and F1, F2-type cycles (Fig. 13) con-

sisting of relatively deeper, coated crinoidal grainstones

and oolitic grainstones with quartz fragments towards the

upper part and the sequence is capped by quartz arenitic

sandstone facies.

The scale of cyclicity in the measured section near

Hadim is comparable to that in the Late Paleozoic sea level

chart of Ross and Ross (1987, 1988), the sequence strati-

graphic chart of the Donets Basin constructed by Izart et al.

(2003) and the main transgressive–regressive sequences of

Davydov et al. (2004). Importantly, however, the position

of the mid-Carboniferous boundary in our study does not

coincide with a sequence boundary as interpreted by other

investigators. Ross and Ross (1987, 1988) considered the

coastal onlap curves of various regions worldwide and

concluded that the mid-Carboniferous boundary falls

between their third-order sequences N3 and N4 (Fig. 14).

In Ross and Ross (1987, 1988), the sequence stratigraphic

placement of the mid-Carboniferous boundary follows

Ramsbottom (1973, 1977, 1979 and 1981) and Ramsbot-

tom et al. (1978) who subdivided the Carboniferous of

England into mesothems, a concept introduced for depo-

sitional sequences larger than cyclothems but smaller than

the ‘sequences’ of Sloss (1963) and close to the deposi-

tional sequence concept of Vail and Mitchum (1977). The

sequence stratigraphic framework of Ramsbottom (1979)

was also used by Izart et al. (2003) who placed the mid-

Carboniferous boundary between their sequences N5 and

Fig. 8 a–b Diplosphearina inequalis, X100, a: HB04-12; b:HB04-

52, c–d Tuberitina sp., X100, c: HB04-45; d: HB04-43, e–hPseudoglomospira spp., X100, e, g: HB04-51; f: HB04-33;

h: HB04-45, i–k Paleonubecularia spp., X100, i: HB04-02;

j: HB04-11; k: HB04-10, l–o Turrispiroides sp., X100, l, m, o:

HB04-16; n: 08, P Paleotextularia sp., X40, HB04-39, q Climacam-mina sp., X40, HB04-11, r Cribrostomum? sp., X40, HB04-45,

s Tetrataxis sp., X100, HB04-30, t Endotaxis sp., X100, HB04-08,

u–w Insolentitheca horrida (=syzgial cyst of different authors.

For references, see Vachard and Cozar 2004), X80, u: HB04-01;

v: HB04-09; w: HB04-11

c

Facies

123

Facies

123

N6. According to Izart et al. (2003), the mid-Carboniferous

boundary also coincides with the boundary between SS5

and SB1 of their fourth or third-order depositional

sequences in the Donets Basin (Fig. 14). Elsewhere in

Eastern Europe, for example in the Russian Platform and

the Urals, the mid-Carboniferous boundary corresponds to

a gap and cannot be interpreted within a sequence strati-

graphic framework of the region (Alekseev et al. 1996;

Izart et al. 2003). Davydov et al. (2004), by stating that the

Carboniferous cyclic sequences are of glacio-eustatic ori-

gin and therefore global, depicted the mid-Carboniferous

boundary as coinciding with the boundary (Bsh 1) of their

transgressive–regressive depositional cycles in the marine

shallow-water cratonic shelves (Fig. 14).

We suggest here that previous studies placing the mid-

Carboniferous boundary at a sequence boundary are flawed

Table 1 Correlation chart of Upper Serpukhovian to Lower Bashkirian according to Vdovenko et al. (1990), Rui et al. (1996), Shcherbakov

(1997), and Maslo and Vachard (1997)

Russian Platform Donets Basin Urals Western Europe North America In this study

Stages Substages Horizons Horizons Horizons Horizons System Series Horizons

Bashkirian Lower Krasnopolyansky Feninsky Syuransky R (Reticuloceras) Pennsylvanian

(part)

Morrowan Syuransky

Voznesensky Voznesensky Bogdanovsky H (Homoceras) Bogdanovsky

Serpukhovian Upper Zapaltyubinsky Zapaltyubinsky Ustsarbasky E2 (part)

(Eumorphoceras)

Mississippian

(part)

Chesterian Zapaltyubinsky

Table 2 Carbonate and siliciclastic facies and their depositional environments in the studied section

No. Facies type Description Grain types/fossils Position

within

the cycle

Depositional

environment

1 Coated crinoidal

packstone

Bioclastic packstone composed

mainly of crinoids with micritic

envelops

Crinoid fragments, gastropods,

foraminifers, and bivalves

Base Open marine

2 Coated bioclastic

grainstone

Grainstone mainly composed of

skeletal grains with micritic

envelopes or biogenic

encrustations

Foraminifers, crinoids and

echinoid fragments, gastropods,

pelloids, lumps and bioclasts

Base–

middle

Sand shoals (shoal)

3 Oolitic grainstone Grainstone with oolites and

bioclasts

Foraminifers, bioclasts, crinoids

and echinoid fragments, and

gastropods

Base–

middle

Sand shoals (shoal)

Grainstone with radial-fibrous

oolites and quartz grains (*5%)

Oolites with radial structure and

quartz grain

Top Restricted environment

(shoal)

4 Oolitic packstone-

grainstone

Packstone to grainstone composed

of oolites and skeletal grains

Crinoids and echinoid fragments,

peloids, dark intraclasts, lumps,

foraminifers and gastropods

Top–

middle

Sand shoals (shoal)

5 Intraclastic grainstone Grainstone consisting of mainly

intraclasts, lumps, and dark

clasts.

Foraminifers, intraclasts, lumps

and micritized grains

Middle–top Restricted Platform

Interior

(Shoal)

6 Mudstone-wackestone No fossils or few fossils,

homogenous lime mud

Unfossiliferous Top Lagoon platform interior

(lagoonal—restricted)

7 Quartz-peloid grainstone Peloidal packstone which contains

*25% quartz grains

Peloids and quartz grains Base Peritidal (landward side)

8 Quartz arenitic sandstone Sandstone composed very fine

sand to silt-sized quartz grains

Quartz grains, unfossiliferous Top Peritidal (landward side)

Fig. 9 Photomicrographs of microfacies determined in the measured

section. Scale bar is 0.5 mm in length and valid for each photograph,

a–b coated crinoidal packstone (sample HB 09), c–d coated bioclastic

grainstone (sample HB 47), e oolitic grainstone with dominantly

bioclasts (sample HB 41), f oolitic grainstone with quartz grains

(sample HB 20), g oolitic grainstone-packstone (sample HB 21),

h intraclastic grainstone (sample HB 49)

c

Facies

123

Facies

123

by incorrectly integrating biostratigraphic datums within

the sequence stratigraphic framework. Our study based on

bed-scale sampling, stacking patterns of parasequences,

and clearly delineated sequence boundaries suggests that

the mid-Carboniferous boundary does not coincide with a

sequence boundary and is located within a transgressive

systems tract, approximately 3 m above the sequence

boundary.

Fig. 10 Photomicrographs of microfacies determined in the mea-

sured section. Scale bar is 0.5 mm in length and valid for

each photograph, a–b mudstone-wackestone (sample HB 03, HB

34), c–d quartz-peloid grainstone (sample HB 53, HB 59), e–f quartz

arenitic sandstone (sample HB 64)

Facies

123

In bed-scale studies carried out at the mid-Carboniferous

GSSP (Lane et al. 1999; Barnet and Wright 2008), the

boundary was found to fall within a depositional sequence.

In Lane et al. (1999), the boundary lies 68 cm above the

sequence boundary and is placed at the transition between

the transgressive systems tract and the regressive systems

tract (Fig. 14). Richards et al. (2002) and Ellwood et al.

(2007) used this boundary within the same sequence

stratigraphic framework for the application of their mag-

neto susceptibility event method and cyclostratigraphy

studies. A similar sequence stratigraphic approach by

Barnet and Wright (2008) enable them to identify the

boundary within their High-Frequency Cycle 4 (Fig. 14).

Haq and Schutter (2008) also concluded that the mid-

Carboniferous boundary lies within one of their High-

Frequency Cycles (Fig. 14).

Fig. 11 Composite model illustrating the microfacies distribution of Serpukhovian—Bashkirian boundary beds in the studied section

Fig. 12 General aspects of

shallowing-upward cycles in the

mid-Carboniferous beds in

Hadim region

Facies

123

Duration of cycles

Stratigraphic cycles of different orders are defined by

duration: first order ([100 my), second order (10–100 my),

third order (1–10 my), fourth order (0.1–1 my) and fifth

order (0.01–0.1 my) (Goldhammer et al. 1990, 1993;

Lehrmann and Goldhammer 1999). High-frequency fourth,

fifth, or higher order shallowing-upward depositional

cycles are the building blocks of lower-frequency (third-

order) depositional sequences in carbonates (Goldhammer

et al. 1990; Read 1995). Climatic variations result from

cyclic changes in the earth’s orbital parameters such as

Fig. 13 Columnar section showing meter-scale shallowing-upward cycles and sequences (SB sequence boundary, mfs maximum flooding

surface. For parasequence symbols see Fig. 12)

Facies

123

eccentricity, obliquity, and precession. Quaternary eccen-

tricity varies at periods of about 100 ky and 400 ky,

whereas precession cycles have dominant periodicities of

approximately 23 ky and 19 ky and obliquity cycles have

periodicities of about 41 ky. Collier et al. (1990) based on

their computer simulations of coastline movement that

illustrate the interaction of the tectonic subsidence, depo-

sition and eustasy estimated that Carboniferous precession

had periodicities of approximately 19.5 ky and 16.6 ky and

obliquity had a period of 31.1 ky.

The time interval represented by strata at the studied

section is approximately 2 my by comparison with cor-

relative cycles and horizon boundaries in the Donets Basin

identified by Izart et al. (2003). Considering facies evolu-

tion and stacking patterns in the Tauride section, 18 shal-

lowing-upward cycles (parasequences) are identified

between correlated levels. Dividing the time span of 2 my

by the number of cycles, the average duration of a cycle

was calculated approximately as 100 ky.

Cyclic sedimentation has been documented in Carbon-

iferous strata worldwide and has been attributed to sea-

level fluctuations driven by climatic changes (Ross and

Ross 1987; Read 1995). The higher-frequency cycles are

caused by the waxing and waning of polar ice-caps

(Read 1995; Lever 2004) and many studies (Fischer 1984;

Gonzalez 1990; Frakes et al. 1992; Eyles et al. 1993;

Garzanti and Sciunnach 1997; Mii et al. 1999; Miller and

Eriksson 2000; Smith and Read 2000; Wright and Van-

stone 2001; Izart et al. 2003; Rygel et al. 2008; Haq and

Schutter 2008; Barnet and Wright 2008) indicate that the

Serpukhovian—Bashkirian interval occurred during an

episode of glacial activity. Periods with glacial icehouse

climatic conditions are characterized by high-amplitude

change in sea level (Veevers and Powell 1987; Read 1995;

Rankey 1999) driven by the 100 ky cyclicity of eccentricity

(House 1995; Read 1995). In this study, 100-ky meter-scale

cycles lead us to conclude that the cyclicity was glacio-

eustatically controlled eccentricity cycle.

Conclusions

A stratigraphic section in the Hadim region of the Central

Taurides is characterized mainly by carbonate deposits

intercalated with quartz arenitic sandstones. High-resolu-

tion foraminiferal biostratigraphy allows identification of

the mid-Carboniferous boundary and four biostratigraphic

zones. The upper Serpukhovian part of the section is

assigned to the Eostaffella ex gr. ikensis—E. postmosqu-

ensis zone and correlated with the Zapaltyubinsky Horizon.

The lower Bashkirian part of the section is divided into

three zones, namely Plectostaffella bogdanovkensis—

P. jakhensis Zone, Millerella marblensis Zone and Semi-

staffella sp. Zone. These zones allow correlation to the

lower Bogdanovsky, upper Bogdanovsky and Syuransky

horizons, respectively. The mid-Carboniferous boundary

lies between Eostaffella ex gr. ikensis—E. postmosquensis

Zone and Plectostaffella jakhensis—P. bogdanovkensis

Zone.

The mid-Carboniferous boundary beds comprise various

siliciclastic and carbonate microfacies types whose stack-

ing patterns represent shallowing upward cycles. Based on

their texture and composition the studied subtidal shallow-

water carbonate succession is differentiated into eight mi-

crofacies types interpreted to have accumulated in four

depositional belts. Vertical associations among the mi-

crofacies types allow for the recognition of six different

(A–F) cycles and two sedimentary depositional sequences.

The duration of meter-scale cycles was calculated as

approximately 100 ky that corresponds to eccentricity

cycles which are dominant during icehouse periods such as

the Mississippian-Pennsylvanian transition (House 1995;

Read 1995).

The mid-Carboniferous boundary in the studied section

does not coincide with the sequence boundary, but lies

approximately 3 m above a sequence boundary within a

transgressive systems tract. In contrast, many previous

studies have placed the mid-Carboniferous boundary at a

Fig. 14 Correlation of the sequence stratigraphic interpretations of different authors around the mid-Carboniferous boundary

Facies

123

sequence boundary. This discrepancy arises because in

many cratonic areas, the mid-Carboniferous boundary

coincides with a subaerial exposure surface at which there

was a lengthy hiatus. Our results are consistent with

investigations of the mid-Carboniferous boundary in dee-

per shelf and basinal settings, such as the Arrow Canyon

GSSP, where the transition was preserved by continuous

sedimentation (Lane et al. 1999; Richards et al. 2002;

Bishop et al. 2009 and the references therein). The sea-

level chart of Haq and Schutter (2008) correctly places the

boundary within a depositional sequence.

Acknowledgments The authors are thankful to John Groves for his

useful remarks on an earlier version of the manuscript. The editor of

FACIES and the referees, Daniel Vachard and Pedro Cozar, are also

acknowledged for their constructive reviews.

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