1 Sel¸uk Uni ver sity, Fac ulty of En gi neer ing, De part ment of Geo log i cal En gi neer ing, Alaeddin Keykubat Kampüsü, Sel¸uklu, Konya, Tur key
2 Bul gar ian Acad emy of Sci ence, In sti tute of Ge ol ogy, Acad. G. Bonchev bl. 24, 1113, So fia, Bul garia
3 Gen eral Di rec tor ate of Min eral Re search and Ex plo ra tion (MTA), De part ment of Geo log i cal Re search, Üniversiteler Mahallesi DumlupÏnar BulvarÏ No: 139, Çankaya, An kara, Tur key
Okuyucu C., Ivanova D., Bedi Y. and Ergen A. (2014) Dis cov ery of an ear li est Tri as sic, post-ex tinc tion foraminiferal as sem - blage above the Perm ian-Tri as sic bound ary, Strandzha nappes, north-west Tur key. Geo log i cal Quar terly, 58 (1): 117–124, doi: 10.7306/gq.1145
A new foraminiferal fauna from Early Tri as sic (Induan) strata of the ÇaÈlayÏk sec tion on the “Strandzha Mas sif”, north-west Tur key, com prises five spe cies pre cisely de ter mined and five spe cies in open no men cla ture be long ing to ten gen era. They be long to the post-ex tinc tion foraminiferal as sem blage of the Perm ian-Tri as sic cri sis, char ac ter ized by the pres ence of both di sas ter taxa (Earlandia and Postcladella kalhori) and Laz a rus taxa (Diplosphaerina inaequalis, ?Rectostipulina quadrata, Arenovidalina sp. and Glomospira sp.). The pres ent study at Tütünlüktepe For ma tion iden ti fied for the first time the Perm ian foraminifers on the Strandzha Mas sif as rel ict mem bers of a post-ex tinc tion foraminiferal as sem blage.
Key words: Perm ian-Tri as sic bound ary, post ex tinc tion, foraminifera, Strandzha, Tur key.
INTRODUCTION
The “Strandzha Mas sif” or the Istranca Com pos ite Terrane (Hagdorn and GöncüoÈlu, 2007) is one of the com plex tec tonic units or ter ranes in Bul garia and Tur key that cov ers al most 1200 km2 across the Turk ish-Bul gar ian bor der. The struc tural prop er ties and geo log i cal set tings of the Strandzha Terrane have been re cently re viewed in some de tail by Bul gar ian (Gerdjikov, 2005a, b; Dabovski and Zagorchev, 2009) and Turk ish (Okay et al., 2001) re search ers. The first geo log i cal study on the Turk ish part of the “Strandzha Mas sif” was car ried out by Pamir and Baykal (1947). Later, some gen eral geo log i cal stud ies were re al ized in the “mas sif” by ܺümezsoy (1982) and AydÏn (1974, 1982). Ac cord ing to the re cent clas si fi ca tion of Okay and Yurtsever (2006) the “Strandzha Mas sif” which ex - tends along the Black Sea coast is com prised of two main geo - log i cal units, be ing meta mor phic rocks of the “Strandzha Mas - sif” and the Thrace Ba sin. The crys tal line rocks of the
“Strandzha Mas sif” have been clas si fied in three main groups by pre vi ous re search ers: a) low and high grade basal meta mor - phic rocks, b) plutonic rocks that be long to the base ment and c)
Tri as sic and Ju ras sic meta-sed i men tary rocks which form the cover suc ces sion. Re cent stud ies, car ried out both in the Bul - gar ian and Turk ish parts of the “Strandzha Mas sif”, have shown the pres ence of nappe struc tures in the “mas sif” (ªengör et al., 1984; Okay et al., 2001; Gerdjikov, 2005a, b). Re cently, Bedi et al. (2013) rec og nized dif fer ent nappe struc tures in the Turk ish part of the “Strandzha Mas sif”.
We dis cov ered Early Tri as sic foraminifera in recrystallised lime stones to the south-east of ÇaÈlayÏk vil lage (Fig. 1) and found the ev i dence for a post-ex tinc tion foraminiferal as sem - blage above the Perm ian-Tri as sic bound ary.
The Perm ian-Tri as sic mass ex tinc tion event was the most se vere of the Phanerozoic mass ex tinc tions (Erwin, 1993) with more than 90% of ma rine spe cies elim i nated be cause of the de - struc tion of the ma rine eco sys tem (Jin et al., 2000; Bambach et al., 2002). Po ten tial causes and ef fects of the end-Perm ian mass ex tinc tion have been pro posed re main in de bate. Trig gers such as a bo lide im pact, vol ca nic erup tions, oce anic an oxia, rapid cli - mate change, cat a strophic re lease of seafloor meth ane and so on (Baud et al., 1989; Erwin, 1993, 2006; Wignall and Twitchett, 1996; Hal lam and Wignall, 1999; Becker et al., 2001; Kaiho et al., 2001; Weidlich et al., 2003; Knoll et al., 2007) have been sug - gested as the most likely causes for this cri sis.
The foraminifers are one of the most im por tant fos sil groups through the P-Tr tran si tion be cause they are very com mon and dis trib uted in a va ri ety of fa cies set tings. They en able un der - stand ing of bi otic ex tinc tion pat tern via quan ti ta tive anal y sis and their evo lu tion ary his tory across the P-Tr tran si tion (Rampino and Adler, 1998; Jin et al., 2000; Groves et al., 2005; Song et al., 2009a, b, 2013)
* Corresponding author, e-mail: okuyucucengiz@gmail.com Received: August 6, 2013; accepted: November 4, 2013; first published online: January 15, 2014
A sec tion of recrystallised lime stones is well-ex posed in the Turk ish part of the “Strandzha Mas sif” and up un til now has not been found in Bul garia where Early Tri as sic foraminifera- bear ing recrystallised lime stones have only been doc u mented by Trifo - nova (1978, 1984, 1992, 1993, 1994), Chatalov and Trifo nova (1985) and Chatalov (1990) from the Peri-Tethyan (Subb alka - nide) type (Sveti Ilija Ridge) and Tethyan (Stran dzha) type Tri as - sic of Strandzha Moun tain (south-east Bul garia). In the lime - stones be long ing to the Omarcevo For ma tion (Sveti Ilija Ridge), the Lower Tri as sic Meandrospira pusilla acme-zone with a char - ac ter is tic of the Spathian Stage fora miniferal as so ci a tion has been rec og nized. The spe cies Meandrospira pusilla (Brönni - mann), Areno vidalina chialingchiangensis (Ho), Cyclogyra ma - ha jeri Bro ennimann, Zaninetti and Bozor gnia, Kamurana chata - lovi Trifonova, Ammodiscus multivo lutus (Reitlinger), and Glo - mo spira sinensis Ho have been de ter mined and fig ured. In the Tethyan (Strandzha) type Tri as sic the Lower Tri as sic cor re - sponds to the lower and mid dle part of the Goljamo Bukovo For - ma tion (Chatalov and Trifonova, 1985) where only few foramini - fera spe cies have been found, such as Meandrospira pusilla (Ho), Nodosinella cf. rostrata Trifonova, Ammodiscus sp., and Nodosaria sp. The aim of this study is to doc u ment the Early Tri - as sic foraminifers (Induan) and to show the first post-ex tinc tion foraminiferal as sem blage above the P-Tr tran si tion in the Stran - dzha Nappes, north-west Tur key. Thus, the newly found fora - mini fers pro vide some in sights into Early Tri as sic bio stratigraphy and the foraminiferal ex tinc tion pat tern across the P-Tr tran si tion.
GEOLOGICAL SETTING
Re cent stud ies along the Turk ish-Bul gar ian bor der have shown the pres ence of tec tonic units which com pletely dif fer in
stra tig ra phy, li thol ogy and meta mor phic fea tures, and have re - vealed their thrust con tacts be tween them (Bedi et al., 2013).
These struc tural units in Tur key are called the Sarpdere Nappe (Subbalkanide type Tri as sic of Chatalov, 1980), the MahyadaÈ Nappe (Strandzha type Tri as sic of Chatalov, 1980) and the DoÈanköy Nappe (Sakar type Tri as sic of Chatalov, 1980) in as cend ing or der. These three nappes are sealed by Lower Ju ras sic siliciclastic de pos its.
The Early Tri as sic foraminifera in the recrystallised lime - stones were dis cov ered in the Tütünlüktepe For ma tion of the MahyadaÈ Nappe (Fig. 2) which is com posed of De vo nian (?)-Tri as sic suc ces sions. The low er most Pa leo zoic suc ces - sion of the MahyadaÈ Nappe is De vo nian (?)-Perm ian in age and is called the Armutveren For ma tion. The Armutveren For - ma tion is com posed of in ter ca la tions of red dish, yel low ish, thin-bed ded quartz ite and calc-schist, do lo mite and recry - stallised lime stone. The Tütünlüktepe For ma tion, which is 10-m-thick, dis plays dis con tin u ous out crops in the Turk ish part of the “Strandzha Mas sif” and com prises in ter ca la tions of grey, dark grey, thin- to me dium – and reg u larly-bed ded recry - stallised lime stone and green, thinly fo li ated metasiltstone.
This unit is ob served around Tütünlüktepe Hill only on the road be tween Dereköy-ÇaÈlayÏk in the Turk ish por tion of the
“Strandzha Mas sif”. The Tütünlüktepe For ma tion is un der lain con form ably by the De vo nian (?)-Perm ian Armutveren For ma - tion (Figs. 2 and 3). The Tütünlüktepe and the Armutveren for - ma tions are over lain with an gu lar un con formity by the Early Tri as sic ÇukurpÏnar For ma tion which is equiv a lent the the Struvnitsa For ma tion of Chatalov (1985) in Bul garia and com - posed of metasiltstone, metaconglomerate with quartz schist interbeds, metamicroconglomerate and coarse-grained meta - sandstone. The Mid dle-Up per Tri as sic Adatepe, Tolpan, Kalina Chuka, Kaynakdere and KarlÏk for ma tions are the suc - ceed ing units of MahyadaÈ Nappe (Fig. 2).
Fig. 1. Geo graph ical and the geo log i cal map of the study area and lo ca tion of the ÇaÈlayÏk sec tion (af ter Bedi, 2009)
MATERIAL
Twenty-five sam ples from the ÇaÈlayÏk sec tion (KÏrklareli, south-east of ÇaÈlayÏk vil lage) were col lected from the recry - stallised lime stones, dolomitic lime stones and metasiltstones ex posed there (Fig. 4). Dolomitic and recrystallised lime stones lev els are rel a tively rich in foraminiferal as sem blages and rep - re sented by well- pre served spec i mens (Figs. 5 and 6). The col - lected sam ples have been pro cessed for cono donts, but proved bar ren. Thin sec tions of the stud ied ma te rial are de pos - ited in the MTA (Gen eral Di rec tor ate of Min eral Re search and Ex plo ra tion of Tur key) Pa le on tol ogy Di vi sion.
and Arenovidalina chialingchiangensis (Ho). Sam ple 09- KK-216 is rich in foraminifera, in clud ing Hemigo rdius sp., Ammodiscus sp., Arenovidalina chia - lingchiangensis (Ho), Globivalvulina bulloides (Brady), Glomospira sp.,
?Recto stipulina qua drata Jenny-Des - husses, Diplosphae rina inaequalis (Der ville), Earlandia sp. and Postcla - della kalhori (Brönnimann, Zani netti and Bozorgnia). This part of the sec tion is char ac ter ized by the pres ence of two Laz a rus taxa, Diplo sphaerina inae - qualis (Derville) and ?Recto stipulina qua drata Jenny- Des husses and two di - sas ter spe cies Post cladella kalho ri (Brönnimann, Zaninetti and Bozorgnia) and Earlandia sp. This as so ci a tion char ac ter izes the post-ex tinc tion fora - miniferal as sem blage af ter the Perm - ian-Tri as sic mass ex tinc tion and is also pres ent in the up per part of the sec tion.
The palaeo biogeographic dis tri bu tion of these short- lived di sas ter forms is known from the west ern Tethyan area in clud ing It aly, Hun gary, Yu go sla via, Bul garia, Aus tria, Tur key and Iran (Trifo nova, 1978; Rettori, 1995; Ünal et al., 2003; Groves and AltÏner, 2005).
Foraminifers re cov ered from sam ples 09-KK-218 and 09-KK-219 are very rare and they are as signed to only one spe cies, Ammo discus sp. Sam ple 09-KK- 220 in cludes sim i lar spec i mens to those de scribed from 09-KK-216, with Ammodiscus sp., Hemigordius sp., Earlandia sp., Arenovidalina chialingchian gensis (Ho), Postcla - della kalhori (Brönnimann, Zaninetti and Bozorgnia), Glomospira sp. Af ter four bar ren sam ples ?Recto stipulina quadrata Jenny- Deshusses was found in sam ple 09-KK-225. The up per parts of the ÇaÈlayÏk sec tion yielded foraminifers, apart from sam ple 09-KK-226. The foraminiferal as sem blages of sam ple 09-KK- 227, 09-KK-228 and 09-KK-229 are Ammodiscus sp., Hemigordius sp., Diplosphaerina inaequalis (Derville) and Endo - teba? sp. re spec tively. The foraminiferal abun dance of the last sam ples from the recrystallised lime stone level of the sec tion is much smaller than in the un der ly ing beds. Sam ple 10-KK-228 is the only sam ple that shows strongly recrystallised Lower Tri as sic ooids within all stud ied sam ples.
Fig. 2. Gen er al ized strati graphic col umns of the MahyadaÈ Nappe (Bedi et al., 2013)
INTERPRETATION
The char ac ter is tic foraminiferal as sem blage per mits an ex act chronostratigraphic de ter mi na tion for the recry - stallised lime stones, dolomitic lime stones and metasilt - stones of the sec tion (Fig. 6). The foraminiferal as sem - blage of ÇaÈlayÏk sec tion from bot tom to top (10-KK- 214–10-KK-229) com prises only a post-ex tinc tion pop u - la tion char ac ter ized by di sas ter el e ments of the Early Tri as sic Ep och (Induan; Fig. 6).
An other ar gu ment sup port ing the Induan age of the stud ied rocks is the ob ser va tion of the “Lilliput ef fect”
(Urbanek, 1993), a pat tern of size change through ex - tinc tion events. Early Tri as sic an i mal body fos sils and trace fos sils are small rel a tive to those in older and youn - ger in ter vals. Size de creases sharply through the end- Perm ian ex tinc tion event and Perm ian-Tri as sic bound - ary and the small est sizes are en coun tered in the ear li - est Induan (Song et al., 2011). Ac cord ing to the study of Twitchett (2007), all an i mal groups suf fered a size re - duc tion af ter the Late Perm ian ex tinc tion event and the body sizes of these an i mal groups re mained low when com pared to those of ear lier Perm ian or later Tri as sic times. These small est sizes of or gan isms are ob served in parvus and isarcisa zones of the ear li est Induan (Twitchett, 2006).
The low est Tri as sic strata from the dif fer ent Perm - ian-Tri as sic sec tions of the world (e.g., AltÏner et al., 2005;
Groves et al., 2005, 2007; Shen et al., 2006; Haas et al., 2007) are char ac ter ized by mainly dolomitic lime stone, recrystallised lime stone with nu mer ous tiny foraminifers and reg u lar and pla nar milli metre-scale lami na tions with abun dant py rite crys tals as in the ÇaÈlayÏk sec tion (Fig.
7). The oc cur rence of py rite-rich lithofacies in Perm - ian-Tri as sic bound ary suc ces sions is ev i dence for wide - spread an oxia in shal low ma rine en vi ron ments dur ing the end- Perm ian mass ex tinc tion (Wignall and Hal lam 1992, 1993; Wignall and Twitchett, 1996).
DISCUSSION
In the ÇaÈlayÏk sec tion, the re cov ered foraminiferal fauna is mainly rep re sented by spec i mens of the gen era Diplospha erina, Arenovidalina, Globivalvulina, Earlan - dia, Hemigordius, Rectostipulina and Postcladella. The de ter mined taxa in clude com mon el e ments of the Late Perm ian and the Early Tri as sic. The foraminiferal as - sem blage of both time in ter vals broadly in di cates the Fig. 3. Geo log i cal cross-sec tions show ing the con tact re la tion ships be tween un der ly ing
and over ly ing suc ces sions of the Tütünlüktepe For ma tion
Fig. 4. Strati graphi cal sec tion of the ÇaÈlayÏk sec tion, show ing the sam pling lev els and li thol ogy
Fig. 5. Foraminifers of the ÇaÈlayÏk sec tion
A–C – Diplosphaerina inaequalis (Derville) (A, B – 09-KK-216, C – 09-KK-229); D–F – Earlandia sp. (09-KK-216); G–N – Hemigordius spp. (G–N – 09-KK-216, N – 09-KK-220); O–S – Ammodiscus spp. (O – 09-KK-227, P–S – 09-KK-216); T–Z – Arenovidalina chialingchiangensis (Ho) (T–X – 09-KK-216, Y – 09-KK-220, Z – 09-KK-215); Aa–Cc – Postcladella kalhori (Brönniman, Zaninetti and Bozorgnia) (Aa, Cc – 09-KK-216, Bb – 09-KK-220); Dd, Ee – ?Rectostipulina quadrata Jenny-Deshusses (Dd – 09-KK-225, Ee – 09-KK-216); Ff – Globivalvulina bulloides (Brady) (09-KK-216); Gg–Ii – Glomospira sp. (09-KK-220); Jj – Endoteba ? sp. (09-KK-228); scale bar is 20 mm
end-Perm ian mass ex tinc tion and its di sas ter, sur vi vor and af - ter math com po nents.
The Perm ian rel ict foraminifers con sist of Globivalvulina bulloides (Brady), Diplosphaerina inaequalis (Derville), ?Recto - stipulina quadrata Jenny-Deshusses and Hemigordius sp.
Globi valvulina bulloides (Brady) is very com mon in Perm ian strata but also oc cur in low er most Tri as sic suc ces sions as a sur vi vor of the Perm ian-Tri as sic mass ex tinc tion (e.g., Bed 27, Meishan sec tion from the south ern China; Song et al., 2009a).
These taxa show many sim i lar i ties to those of the Meishan sec - tion “Sur vival Fauna Beds” (Bed 25–27; Chen et al., 2006) and com pare with those of the sec ond ep i sode of ex tinc tion (Song et al., 2007). These Perm ian rel ict fau nas have been de scribed to gether with the ear li est Tri as sic foraminifers such as Postcla - della kalhori (Brönnimann, Zaninetti and Bozorgnia) and Areno -
vidalina chialingchiangensis (Ho). Postcladella kalhori (Brönni - mann, Zaninetti and Bozorgnia) (with the type spe cies Recto - cornuspira kalhori Brönnimann, Zaninetti and Bozorgnia) is well-pre sented in the stud ied ma te rial. Krainer and Vachard (2011) rec og nized that Cornuspira? mahajeri and Rectocornu - spira kalhori be long to the same ge nus and in tro duced the taxon as Postcladella kalhori n. comb. The known strati graphic dis tri bu tion of Postcladella kalhori is from lat est Mid dle Perm ian to ear li est Tri as sic strata; it is es pe cially com mon and char ac - ter is tic of Induan (ear li est Tri as sic) strata glob ally, for in stance, in South China (Ezaki et al., 2003; Song et al., 2007, 2009b;
Galfetti et al., 2008), south ern Tur key (Crasquin-Soleau et al., 2004; AltÏner et al., 2005; Groves et al., 2005; Payne et al., 2007) and north ern It aly (Groves et al., 2007). Some ques tion - able oc cur rences of this taxon are in di cated in the Olenekian (late Early Tri as sic; Krainer and Vachard, 2011). Rep re sen ta - tives of the ge nus Earlandia are known from the level above the P-Tr mass ex tinc tion ho ri zon in South China (Ezaki et al., 2003;
Song et al., 2007, 2009a, b), south ern Tur key (AltÏner et al., 2005; Groves et al., 2005; Angiolini et al., 2007), It aly (Groves et al., 2007) and Hun gary (Hips and Haas, 2006). Postcladella kalhori and Earlandia oc cur to gether with in ferred di sas ter taxa foraminifer in the af ter math of the P-Tr cri sis (Hal lam and Wignall, 1997; Groves and AltÏner, 2005; Groves et al., 2005, 2007; Song et al., 2007, 2009a, b).
The ge nus Arenovidalina is in ter preted as a Laz a rus taxon by Zaninetti et al. (1992), Rettori (1995), AltÏner et al. (2005) and Groves and AltÏner (2005) and its oc cur rence in Early Tri as sic (Induan?-Olenekian stages) prob a bly rep re sents a phyle tic con tin u a tion of Perm ian forms as signed to Neohemi gordius (AltÏner et al., 2005). Based on pub lished data (AltÏner et al., 2005; Groves and AltÏner, 2005; Song et al., 2011) the known strati graphic range of Arenovidalina chialingchiangensis (Ho) is from the Olenekian (Early Tri as sic) to Anisian (Mid dle Tri as sic).
The suc ces sions from the ÇaÈlayÏk sec tion are thin over all be cause of the lim ited ex po sures of the Tütünlüktepe For ma tion which is 10-m-thick in the Turk ish part of the “Strandzha Mas sif”
and has no ex po sure in the Bul gar ian part. The un der ly ing and Fig. 6. Strati graphic oc cur rences of foraminifers
in the ÇaÈlayÏk sec tion
Fig. 7. Oc cur rences of py rite cubes in the dolomitic lime stone lev els
A – sam ple 09-KK-216; B – sam ple 09-KK-228
Five spe cies and five spe cies in open no men cla ture be long - ing to ten gen era of the cal car e ous foraminifers were dis cov - ered in recrystallised lime stones to the south-east of ÇaÈlayÏk vil lage on the “Strandzha Mas sif”. The foraminifera dis cov ered rep re sent a post-ex tinc tion pop u la tion of Induan stage (Early
log i cal In sti tute of the Bul gar ian Acad emy of Sci ences (BAS).
The au thors would like to ex tent their thanks to the both part - ner’s pro ject mem bers for their con tri bu tions dur ing the field work. We also thank R. Rettori and H. Song and the jour nal ed i - tor T. Peryt for their con struc tive and help ful com ments that helped to im prove the manu script sig nif i cantly.
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