CAMBRIAN

M. Cemal GÖNCÜOĞLU1, Olaf ELICKI2, Hüseyin KOZLU3, Semih GÜRSU4

1 Middle East Technical University, Department of Geological Eng., Ankara-Turkey

2 Freiberg University, Geological Institute, Freiberg, Germany

3 Çiğdem Mah.1575 Sok. 41/22-Cankaya/Ankara-Turkey

4 Muğla University, Department of Geological Eng., Kötekli-Muğla-Turkey

INTRODUCTION

A number of the crystalline rocks with Cambrian radiometric ages are reported in the

northern Istanbul-Zonguldak Terrane. Other than in the southern terranes, these arc-

type granodiorites intrude or are associated with Late Neoproterozoic metagabbros,

orthoamphibolites and pyroxenites (Ustaömer and Rogers, 1999). Overall, the

Cambrian rocks are interpreted as representatives of a Cadomian intra-oceanic arc,

formed within the Iapetus-Tornquist oceanic lithosphere (Göncüoğlu, 1997;

Göncüoğlu and Kozlu, 1997).

In some successions in the Menderes Massif and the Central Anatolian Crystalline

complex of the Anatolides, rock units very similar to those in the Tauride-Anatolide

platform are reported by Kozlu and Göncüoğlu (1997). The Cambrian in the Taurides

shows in general very similar features across the belt (Figure 1) and will be evaluated

in detail in the following chapters.

Figure 1: Correlation of the Cambrian successions in the Taurides (modified after Göncüoğlu,

1997)

In the SE Anatolian Autochthon the Cambrian rocks are represented by the Sadan

(=Zabuk), Koruk and Sosink formations, respectively. The Sadan Formation is

transgressive on the pre-Cambrian fluvial sediments and volcanic rocks. The

geological evolution of the Cambrian has been recently reviewed by Ghienne et al.

(2010 and the references therein) and briefly summarized by Kozlu and Ghienne (this

volume) in the following chapter. This recent evaluation of these authors suggests

that in ascending order the following depositional sequences can be distinguished on

the basis of recognition of major transgressive events and subsequent shelf

progradations. The first one is earliest Cambrian (early Terreneuvian) in age and

corresponds to the initiation of a cratonic platform regime upon a Late Neoproterozoic

basement with bimodal volcanism (Gürsu et al., 2010). The deposits are alluvial fan,

lagoonal and lake and playa type in ascending order. Very recently Demircan et al.

(2011) reported ichnofossils of Terreneuvian Series in this unit. The second

depositional sequence is late Terreneuvian? to early Furongian (early Cambrian to

early Late Cambrian in the former terminology) in age, whereas the third one includes

the late Furongian to early Middle Ordovician (Late Cambrian to middle Arenig in the

British regional terminology) interval. These two sequences are related to the

development of a stable platform, represented by the deposition of fluvial to tidal

siltstones and sandstones (Sadan Formation) shallow marine carbonates (Koruk

Formation in SE Anatolian Autochthon), and the Çal Tepe formation in the Taurides

(Figure 2). The succession comprises dolomite-limestone-nodular limestone in

ascending order and is relatively well-dated by trilobites and chitinozoans (Dean and

Monod, 1997; Ghienne et al., 2010).

The third depositional sequence is characterized by the storm-dominated, essentially

carbonate-free, detrital deposits constituting the Sosink Formation in the SE

Anatolian Autochthon and the Seydişehir Formation in the Taurides (Dean and

Monod 1990). The biostratigraphic control is based on trilobites and acritarchs (Dean

and Martin 1992, Paris et al., 2007).

The classification may also help for a reliable correlation between the Turkish and

Arabian Lower Paleozoic formations as given in Figure 3.

Figure 2 : Depositional features and distribution of the Middle and Late Cambrian in the Taurides and the SE Anatolian Autochthon (Ghienne et al., 2010).

CAMBRIAN STRATA IN THE TAURIDES

Western and Central Taurides

In the western Central Anatolia, Cambrian rocks disconformably overlie the

Neoproterozoic “Sandıklı Basement Complex” (Gürsu and Göncüoğlu 2001). The

Basement Complex is composed of siliciclastic rocks with rare black chert and

dolomite lenses and includes conglomerates, dark colored brecciated limestones,

cherty and laminated limestones interbedded with sandstones. This low-grade

metamorphic unit is intruded by porphyroids and microgranites with latest

Neoproterozoic zircon ages (Gürsu et al., 2004), which in turn are unconformably

overlain by variegated conglomeratic sandstones and shales with basic to

intermediate lava flows.

Upwards, they grade into green, violet and yellow quartz siltstones (Göğebakan

Formation, Figure 4) and variegated mudstones. They are transgressively overlain by

tidal-dominated deltaic sandstones, siltstones and rare shales (Celiloğlu Member)

Figure 3: Tentative correlation of Cambro-Ordovician successions in the Near and the Middle East and N Africa with special emphasise on the Middle Cambrian Çal Tepe Formation (Elicki et al., 2012).

that have yielded Early Cambrian trace fossils (Erdoğan et al., 2004). The overlying

tidal sandstones (Hüdai and Feke formations) are very widespread throughout the

Taurides. They are conformably overlain by the Çal Tepe Formation. The Çal Tepe

Formation forms a trilogy of dolomite-dolomitic limestone, black limestone and

nodular limestone. It starts with inter-to shallow subtidal, partly restricted-marine

carbonates, followed by subtidal to deep-subtidal, open marine limestones with

microbial formations. The nodular limestones are condensed and open marine. It

includes microbial-archeocyathan biostromes. The ages and fossil contents are

shown on Figure 5.

Figure 4: Generalized Columnar Section of the Cambro-Ordovician rocks in Sandıklı area (After Gürsu et al., 2004 and Elicki et al., 2012).

Figure 5: Ages and fossil content of the Çal Tepe Formation (Elicki et al., 2012)

In the type-section of the Çal Tepe Formation in the Seydişehir area (Figure 6), only

the Çal Tepe formation and its transition to the overlying Seydişehir Formation are

observed. Here again the dolomite- black limestone/light gray limestone-nodular

limestone subdivision is very well established and had been relatively well-studied

considering its biostratigraphy (Sarmiento et al., 2001; Dean, 2005; Elicki et al., 2007;

Elicki and Gürsu, 2009)

Figure 6: Cross section of the Çal Tepe Formation in its type-locality (after Dean, 2005 and Elicki and Gürsu, 2009)

Further Cambrian outcrops in the W and Central Taurides are reported in the

Tahtalıdağ (Şenel et al., 2000), Antalya-Kemer (Göncüoğlu and Kozur, 1999), Silifke-

Ovacık and Alanya-Anamur (Demirtaşlı, 1984), Sultan Mountains (Shergold & Sduzy,

1984) and Sarıçiçek (Dumont, 1972) regions and correlated in Figure 1.

CAMBRIAN IN THE EASTERN TAURIDES

The Cambrian rocks in the Eastern Taurides are mainly represented by two

formations in the Geyikdağı Unit of Özgül (1976) The lower one is represented by

quartzites and quartz-arenites, variably called as the Koçyazı (Özgül and Kozlu,

1993) or Feke Quartzite (Kozlu and Göncüoğlu, 1997). It is the equivalent of the

Hüdai Formation in the W and Central Taurides. It conformably overlies a very thick

basement succession made of siliciclastic rocks cut by felsic dykes, black and gray

shales, lydites (Oruçlu Member) and stromatolitic, ankeritic and cherty limestones

and dolomites (İçmetepe Member). The unit was named as the Emirgazi Formation

by Özgül et al. (1972) and well-exposed along numerous sections in the Kozan,

Feke, Tufanbeyli and Saimbeyli areas (Figure 1) in the Geyikdağı Unit of the E

Taurides. The illite crystallinity (IC) value of the white micas of the Emirgazi

Formation is <0.25 indicating to epimetamorphic conditions prior to the deposition of

the overlying Cambrian rocks (Bozkaya et al., 2002).

Feke Quartzite Formation

This unit was also named as the Koçyazı Formation of the Emirgazi Group by

Özgül and Kozlu (2002). The Feke Quartzite transgressively overlies the Kozan

Formation. The type locality is to the north of the town Feke, where the measured

thickness of the unit reaches up to 600 metres. Despite lateral thickness variations,

the Feke Quartzite Formation can be traced all along the Eastern Tauride Belt

(Figure 1). The formation rests with an 12 to 40 m thick coarse sandstone –

conglomerate level on the İçmetepe Member of the Kozan Formation (Özgül and

Kozlu, 2002). The contact is evaluated as a parallel unconformity.

Upwards, the following part of the formation is represented by an unnamed

member with greenish gray siltstones, sandstones and shales and includes trace

fossils (Figure 7). Upwards it is transitional to the main body, about 400 m thick,

comprising pink to yellow coloured, medium bedded quartzarenites with cross-

lamination and ripple-marks.

The formation correlates with the Hüdai Quartzite, and Zabuk formations, both

synonyms of the Feke Quartzite in the western Taurides (Dean and Özgül 1994) and

SE Anatolia (Kellog 1960), respectively.

Figure 7: Trace fossils in the siltstones-mudstones of the Feke Formation.

Çal Tepe Formation

In the Eastern Taurides an almost 110-m-thick carbonate sequence

conformably overlying the Feke Quartzite Formation was described by Demirtaşlı

(1978) as the Değirmentaş Formation, the equivalent of the Çal Tepe Formation.

Following Dean and Monod (1990), we use the term Çal Tepe Formation to describe

this unit in the entire Tauride Belt.

The formation conformably rests on the Feke Quartzite. The contact, wherever

observed is represented by a carbonate-cemented sandstone, locally with pebbles of

quartz and volcanic rocks (Özgül and Kozlu, 2002). The sandstone is followed by

black stomatolitic dolomites with chert nodules and layers. The rest of the Çal Tepe

Formation in the Eastern Taurides will be the visited in the first two Stops of the Field-

excursion and a detailed account of its lithostratigraphic features is given in the next

chapter.

DEĞİRMENTAŞ-HALEVİKDERE SECTION

STOP 1: ÇAL TEPE LIMESTONE AT DEĞİRMENTAŞ VILLAGE The Cambrian section to be visited outcrops to the NE of Değirmentaş Village and

starts with the Dolomite Member of the Çal Tepe Limestone. It is bounded towards

NW by an important fault zone (Değirmentaş Fault) juxtaposing the Lower Paleozoic

rocks with the Mesozoic-Tertiary carbonates (Figure 8). Hence, the lower part of the

Cambrian succession, namely the Hudai Quartzite in the W Taurides or the Feke

Quartzite in the E Taurides is not represented in this area.

Figure 8: Geological map of the Paleozoic rocks in Halevikdere (modified after Monod et al., 2003).

The stratigraphy of the Çal Tepe Formation in the Değirmentaş section is generally

comparable to the standard subdivision known from the type section area in the

western Taurides (e.g. Dean and Monod, 1980) and includes the Dolomite, Black

Limestone, Light Grey Limestone and Nodular Limestone members. The measured

stratigraphic section of the Çal Tepe Formation at Değirmentaş Village is given in

Figure 9.

Figure 9: Measured stratigraphic section of the Çal Tepe Formation to the N of Değirmentaş

village.

Dolomite Member

The dolomitic portion in the lowermost observable part of the carbonate succession

belongs to the Dolomite Member. The rock is characterised by dolomitic and

dolomitized lithologies with some special expressions. Primary structures are only

rarely visible and consist of indistinct subhorizontal, or sometimes wavy layering and

rare slumping features. In some cases, an interpretation as stromatolitic/microbial

structures seems to be reasonable. Further biogenetic structures could not be

observed. The crystallinity of the rock is sometimes coarse, sometimes fine and is not

strictly bound to the bedding what can be interpreted as a feature of (later)

diagenesis. It seems that a first stage of dolomitization has taken place very early

(“syn-sedimentary”) and a second act of dolomitization has affected the succession

rather late. Diagenetic breccias do also occur. A distinct phenomenon is the

occurrence of thin non-continuous chert-layers (Figure 10). These are up to several

cm thick and show internal bedding features. Nevertheless, the layers are laterally

not consistent and often occur patchy as lenses or spheres up to 30 cm in diameter.

The formation time of this silicification is hard to estimate. Early as well as late

diagenetic origin is possible. For sure, there is no possibility to interpret the chert

layers as primary sedimentary structures. Overall, this member lacks characteristic

features of open-marine deposition and can represent a bedded dolomite suite,

probably formed in a restricted environment with lagoonal microbial (Figure 11)

activity.

Figure 10: Field occurrence of the typical Dolomite Member lithology with massive, but thickly stratified dolomite beds and levels and with distinct diagenetic silicification (pen for scale).

Figure 11: Close-up view of the Dolomite Member lithology showing coarse dolomite with irregular and thin microbial fine-lamination bands (pen for scale).

Black Limestone Member and Light Grey Limestone Member.

Up section it seems that there is no clear differentiation in the two members known

from the type area in the western Taurides. The lithotypes occurring up section (until

the Nodular Limestone Mbr.) are well-bedded and they often show fine bedding and

dark/light-lamination (Figures 12 and 13) in mm-scale as well as re-deposition (grey

lithotypes).

Figure 12: Finely laminated black limestone. Lamination is probably of microbial origin. Note the distinct slumping structure with some brecciation focused in this horizon (pen for scale).

Figure 13: Black limestone with finely laminated texture. Especially at the bottom some microbial texture (bio-lamination) is visible. Note that the thin layer on top does not show any wavy texture (hand lens for scale).

This lamination is characterized by irregular lining pointing to a microbial origin of this

feature. The lack of shelly fossils may support this interpretation. In some horizons a

dark grey to black colour of the rock is well expressed and here, not only the mm-

lamination, but also the occurrence of “birds eyes”-like structures is typical (Figure

14).

Figure 14: Black limestone with elongated "birds eyes"-like structures of microbial origin (top is to the right). These structures are orientated to the bedding and accumulated in distinct levels of few cm to dm (hammer for scale).

The “birds eyes” show clear horizontal orientation and a dependency of their size

according to the bedding horizon. This means that there are cm-thick (horizontal

persisting) levels of one size of “birds eyes” (up to few cm in length and few mm in

height) alternating with levels showing other size of “birds eyes” structures (few mm

in length and about 1 mm in height). The “birds eyes” are filled by sparry calcite

which today shows a fine outer rim and a coarse/blocky interior. This can be

interpreted rather as a feature of secondary re-crystallization than of primary filling

structures. This kind of diagenetic overprint is supported by the sometimes not sharp

boundaries between the “birds eyes” and the surrounding sediment.

Further, the interior structure of calcite crystals is sometimes lamellar and

tilted/twisted, which points to a growing of the crystal under physical stress. Pyrite

crystals do also occur, as well as idiomorphic crystals as framboidal (latter points to

bacterial induced origin under oxygen deficiency conditions).

There is no shelly fossil occurrence in this lithotype. Interestingly, there is an

occurrence of similar lithotype in the Çal Tepe sections at different parts of the

Taurides in the similar lithostratigraphic position, preliminary interpreted as probable

archaeocyathan-like structures. Albeit the texture is quite similar to typical microbial

and archaeocyathan feature, there is no clear indication for such an interpretation in

these sections. So, comparing this lithotype in all these sections, this preliminary

interpretation (archaeocyaths) has to be doubted. In destination to the top, the “birds

eyes”-like structures disappear and lamination, more slumping and brecciation occur.

A further lithotype in the black portion is represented by sparitic limestone with poorly

preserved globoidal structures suggesting similarities to microbial structures

described from other regions as “microbial balls” These are represented by small

(several mm maximum), hollow, irregular, cloud-like structures typical for some

special growth-patterns of microbes. The structures are accumulated in distinct

horizons what may support such an interpretation. Shelly fossil content or “birds

eyes”-like structures (as described above) do not occur, but idiomorphic dolomite and

pyrite crystals do.

A last type of lithology is represented by a sample of dark grey lithoclastic limestone

(Figures 15 and 16). The lithoclasts are very small, elongate and often platy (sub-mm

until few mm thick, and until few mm to 1 cm long). Their shape is often irregular and

sometimes bordered by sutures of pressure solution. The clasts are fully sparitized.

Only indistinctly some shelly remains are visible.

Figure 15: Lithoclastic black limestone with indistinct microbial texture (top is to the left). The lithoclasts are small and mostly platy, and they consist of sparry calcite. Mostly, the clasts are sub-parallel to the bedding, bud sometimes also tilted according to some current (not by bioturbation) activity (pen for scale).

Figure 16: An example for the brecciated black limestone lithotype is the lithoclastic black limestone. Note the orientation of the platy lithoclasts and the cut-outs through massive layers, both interpreted as results of bioturbation typical for very shallow subtidal to intertidal environments (pocket-knife for scale).

Echinoderm sclerites and idiomorphic pyrite crystals occur sporadically. The

lithoclasts are nearly completely oriented parallel to the bedding plane, only some of

them are tilted (but all of them to the same direction, what could be interpreted rather

to a certain current than to a sign of bioturbation). Interestingly, horizons of small-

sized clasts alternate with those of larger size. The lithoclastic limestone occurs

immediately at the boundary to the overlaying Nodular Limestone Member (NLM).

Here, brecciation (Figure 17) seems to be more common. Towards the contact

between the black microbial limestones to the nodular ones, also micro-scale slump

structures, truncations and brecciation (Figure 18) are very common and were

assigned to the onset of extension and deepening, which in turn resulted in a change

in lithology and to an increase of organisms.

Figure 17: Black limestone with microbial, somewhat stromatolitic structures (upper centre) and lithoclasts (e.g. centre). In the lower half of the picture (right) diagenetic brecciation is visible (pen for scale).

Figure 18: Micro-slump structures in the upper part of the brecciated limestone close to the Nodular Limestone Member. The structures are very probably of seismic origin (pen for scale).

Nodular Limestone Member

The lower transition of the Nodular Limestone Member towards the Black Limestone

is sharp (Figure 19).

Figure 19: Lower sharp boundary of the Nodular Limestone Member. To the left there is black limestone with microbial texture, slumping and brecciation. To the right there is nodular limestone with distinct content of silt, conspicuous echinoderm and shelly microfauna. This transition point to a sudden change in the environmental conditions and is interpreted here as induced by tectonic disintegration of the shelf (pen for scale).

The first portion of the NLM is not so much nodular, but rather a diagenetic wavy

alternation of silty stuff and limestone (diagenetic bedding). The most exciting feature

is the (1) change of the colour, (2) the occurrence of siliciclastics material, and (3) the

conspicuous fossil content (disarticulated shelly fossils and echinoderms). The fossil

content is often accumulated/enriched in distinct horizons indicating condensed

deposition for the whole sequence. Over the full succession of the NLM there are

some changes in (1) the colour (reddish/greenish), in (2) the degree of nodularity

(Figures 20 and 21) and in (3) the amount of siliciclastics material. In destination to

the top the siliciclastics proportion does increase distinctly.

From the Nodular Limestone Member all samples taken, one every few metres in

vertical distance, are identified as bioclastic wackestones (limestone) varying in the

characteristics mentioned above. The lower boundary is very sharp, whereas the

upper boundary is transitional.

Near the base of the member, the limestone is characterized by many stylolitic

sutures of pressure solution (parallel to the bedding plane) which led to a

pseudoclastic texture.

Figure 20: Typical nodular limestone of the Nodular Limestone Member (top is to the right). The degree of nodularity of the rock varies. The different colour is caused by variations in the amount of siliciclastics material in the rock and in the degree of cementation by calcite. The same parameters are responsible for (and modify) the typical nodular texture (hammer for scale).

Figure 21: Typical succession of the Nodular Limestone Member. Note the nodularity of the rock (well visible in the centre of the picture) and the more or less regular bedding style (diagenetic bedding). This texture, the bedding and paleontological data (see text) clearly point to a somewhat deeper and more distal depositional environment. The distribution of biota suggests a periodical influence by higher energetic events (storms) and a condensed deposition (hammer for scale).

The fossil content is dominated by mostly irregularly shaped, marginal solved, quite

well preserved and non-oriented echinoderm bricks and plates. The internal net-like

structure typical for echinoderms (stereom) is only rarely preserved (mostly

diagenetically modified into calcite single-crystals). Only rarely, very small columnal

remains with lumen occur. Shelly fossils are mostly not to identify more detailed

because of poor preservation. They are distinctly altered into coarse sparry crystals

(often the sclerite itself is disarticulated into such crystals). No internal structures are

visible, but few remains can be interpreted as trilobites due to typical shape.

Generally, the fossil content fluctuates quantitatively somewhat from layer to layer.

Here, there is no indication of bioturbation.

Few decimetres up section there are stylolites in orthogonal directions that can be

interpreted as influence by another pressure orientation than due to overburden. In

the same direction the echinoderm content decrease a little, whereas the shelly fossil

content (especially the trilobite content) increases. Here additionally, very small,

broken and flow-like orientated shelly remains are nest-like (cluster) accumulated

which is a good indication of distinct amount of bioturbation.

A little more up section the shelly fossil (mainly trilobites) content increases again.

Among the echinoderm remains, stem columnals (small) are a little more common

than below, where they occur rather as plates and bricks. Within the silty layers also

frazzles/clasts of claystone are observable. Bioturbation is well expressed and can

often be observed due to orientation features of components within the rock texture.

Near the upper transition of the NLM, the fossil content is represented by distinct

domination of trilobites, but they are distinctly more delicate than before. Echinoderm

stem sclerites are small and show in one case also a pentagonal lumen. Also here,

bioturbation is present.

Much closer to the transition to the siliciclastics Seydişehir Formation, the amount of

silt increases distinctly. Here, a primary alternation of (greenish) siltstone and

limestone can be observed (several mm to 1 cm alternation). The limestone yields

small and thin shelly remains (predominantly trilobites). But also the somewhat

carbonatic siltstone contains some thin shell remains. Internally, the siltstone shows a

sub-mm layering by fluctuating clay content. The NLM – Seydişehir Formation

boundary is an alternation of nodular limestone bands

Generally it can be stated that from the base to the top of the member the

echinoderm content decreases, whereas those of trilobites and other shelly remains

increases. Nevertheless, trilobites and echinoderms are clearly the dominating

bioclasts, indicating an open marine environment of normal salinity and possibly of

not very shallow conditions (maybe few tens on metres) what is in contrast to the

very shallow and often restricted environments of the succession below. The

increased occurrence of slumping and brecciation at the lower transition to the NLM

indicate a rather sudden change of the shelf stability by probably tectonic reasons,

which is quite similar to the shelf evolution in the western Mediterranean successions

in Perigondwana, too).

STOP 2: DEĞIRMENTAŞ ROAD CUTTINGS

The upper part of the Çal Tepe Formation is well-exposed on the Degirmentaş Road.

Here, the main body of the Cambrian succession is juxtaposed along an important

Neotectonic fault (Değirmentaş Fault on Figure 8) with the Eocene limestones. The

measured stratigraphic section of the upper part of the Çal Tepe Formation is given

in Figure 22.

Figure 22: Measured stratigraphic section of the upper part of the Çal Tepe Formation and the transitional zone to the overlying Seydişehir Formation.

Here, the nodular limestones intercalate with the lower part of the Seydişehir

Formation. They are reddish-violet and may reach up to 8 m in thickness (Figure 23).

The thickest nodular limestone band about 50 m above the base of the measured

section is also a bioclastic wackestone and its facies expression corresponds to what

is typical for the middle to higher (but not the highest) portion of the NLM of Çal Tepe

Formation. The fossil content is not orientated and may probably indicate to

bioturbation. Due to cloudy sparitization a more detailed statement on the textures is

problematic.

Figure 23: Typical succession of the lower part of the Seydişehir Formation (top is to the right). Note the regular bedding of the deeper marine siltstones to sandstones (top is to the right). In some levels nodular limestone (few dm thick and of the same facies as the Nodular Limestone Member of the Çal Tepe Formation below) is intercalated, indicating some fluctuations of the sea-level.

The Dolomite Member in the basal part of the section in STOP 1 is obviously Lower

Cambrian (in classical terms) in age, based on the correlation with other sections of

the Çal Tepe Limestone (see also Figure 5) . The transition to the Middle Cambrian is

probably few meters below the Nodular Limestone Member (which is about middle

Middle Cambrian). The boundary to the Upper Cambrian is probably in the lower part

of the Seydişehir Formation (lowermost layers of them still belong to the Middle

Cambrian). More detailed information is hard to give because the correlative data are

from other regions in the west and in the east, and we have a diachronic nature of

the deposition from west to east.

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