GeolCarp_Vol69_No3_301

GEOLOGICA CARPATHICA

, JUNE 2018, 69, 3, 301–311

doi: 10.1515/geoca-2018-0018

www.geologicacarpathica.com

Calpionellid biostratigraphy and microfacies

of the Upper Tithonian pelagic carbonates

in northeastern Serbia (Carpatho–Balkanides)

IVANA CAREVIĆ



, MORTEZA TAHERPOUR-KHALIL-ABAD

, MONIKA MIRKOVIĆ

VELIMIR JOVANOVIĆ

, ELHAM MOJTAHEDIN

and DRAGANA VUŠKOVIĆ

Faculty of Geography, University of Belgrade, Studentski trg 3/3, 11000 Belgrade, Serbia;



carevic.ivana@gmail.com, icarevic@gef.bg.ac.rs, jocavj@gmail.com

Young Researchers and Elite Club, Mashhad Branch, Islamic Azad University, Mashhad, Iran;

m_taherpour@mshdiau.ac.ir, e.mojtahedin@yahoo.com

Geological Institute of Serbia, Rovinjska St. 12, 11000 Belgrade, Serbia; monika.mirkovic@gzs.gov.rs

University of Niš, Faculty of Science, Višegradska 33, 18000 Niš, Serbia; dragana.maric@gmail.com

(Manuscript received February 10, 2018; accepted in revised form April 23, 2018)

Abstract: The occurrence of microfossil assemblage represented by calpionellids in close association with benthic

foraminifera and encrusting Crescentiella morronensis is reported for the first time from the Upper Tithonian of

NE Serbia. The biostratigraphic and sedimentological investigations were carried out on a 250 m thick carbonate

succession in Jelenska Stena quarry cropping out along the Danube River Gorge in the border area of Serbian Carpatho–

Balkanides and Romanian Southern Carphatians. On the basis of determined benthic foraminiferal taxa Textularia sp.

cf. T. bettenstaedti and Everticyclammina praekelleri in the lower part of the succession and calpionellid association

dominated by the representatives of calpionellid genera Tintinnopsella, Crassicollaria and Calpionella the carbonate

succession is assigned to the Upper Tithonian. The scarcity of calpionellid zonal species prevents the nominal zones being

recognized. Petrographic analysis of thin-sections led to the recognition of three basin microfacies types: bioclastic

wackestone, bioclastic peloidal wackestone/packstone and mudstone. These microfacies characterize the SMF 3 and

SMF 4 which indicate deposition in slope and toe-of-slope environments. This study extends the palaeogeographical

distribution of Upper Tithonian calpionellids along the northern Tethyan margins. The investigated carbonate succession

is compared with coeval strata from other northern Tethyan regions.

Keywords: Getic, Carpatho–Balkanides, northeastern Serbia, calpionellids, benthic foraminifera, Upper Tithonian.

Introduction

The Tithonian pelagic carbonates deposited during the Jurassic/

Cretaceous transition in northern Alpine Tethys environments

have a large extent and thickness in the northern part of Serbian

Carpatho–Balkanides. Grubić & Jankičević (1973) considered

these sediments as a part of the carbonate shelf platform

margin-to-basin transitional environment, which represents

the eastern margins of large carbonate platform, initially

named the “Kučaj‒Tupižnica carbonate paraplatform”. Nowa-

days it is also known as the Getic carbonate platform. During

the Late Jurassic and Early Cretaceous the platform attained

a position from the Romanian–Serbian border in the north

westwards towards the Serbian‒Bulgarian border in the east.

It started its evolution on the northern rim of the Tethys in

the Late Jurassic and end with the formation of “ Urgonian”- type

sediments during the Barremian/Early Aptian. The general

stratigraphy of the further northern parts of the Getic of

Carpatho‒Balkanides was summarized by Sučić-Protić (1961)

and Kalenić et al. (1980). A preliminary report on the pelagic

Upper Jurassic carbonate successions from northeast Serbia

has recently been presented by Carević et al. (2017).

The study area corresponds to the Kučaj terrane, also known

as the Getic tectono-stratigraphic unit and represents the trans-

border area towards the South Carpathians of Romania across

the Danube (Karamata & Krstić 1996; Krstić et al. 1996;

Berza et al. 1998; Bojar et al. 1998; Iancu et al. 2005).

Geotectonically it is also regarded as part of the Kučaj‒Svrljig

tectono-sedimentary zone within the Karpatikum (Anđelković

1978; Anđelković & Nikolić 1974, 1980).

This study aims at presenting the results of biostratigraphic

and carbonate microfacies investigation of the Upper Tithonian

pelagic carbonates that represent early phases of evolution of

the platform-to-basin system in the platform margin sequence.

Data obtained for platform margin-to-slope successions in this

paper has revealed new information on the stratigraphy and on

the form of the basin margin.

Material and methods

The transition from the carbonate platform margin to

the adjacent slope environment is exposed on land in the

Jelenska Stena quarry, Danube River Gorge (21°44’18.3” E,

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44°38’49.4” N). The section is being measured and sampled

(Fig. 1). Limestones have been investigated using 30 thin sec-

tions. Carbonate classification follows the scheme of Dunham

(1962); according to it the section comprises mudstones,

wacke stones, packstones, grainstones and rudstones. Generic

attributions of the calpionellid taxa and biostratigraphic divi-

sion are based on the papers by Reháková (1995); Reháková &

Michalík (1997); Lakova et al. (1999); Petrova et al. (2012).

The thin-sections are housed in the collections at the Faculty

of Geography, University of Belgrade under inventory num-

bers which are referred to in the text.

Stratigraphic background

The Upper Tithonian pelagic succession at Jelenska Stena

quarry overlies the Middle Jurassic sandy limestones and

Oxfordian–Kimmeridgian limestones with cherts (Kalenić et

al. 1980; Carević et al. 2011; Ljubović-Obradović et al. 2011).

It is transgressively overlain by a Berriasian to Hauterivian

carbonate deposits and Barremian/Early Aptian Urgonian

lime stones (Carević et al. 2013).

In the Jelenska Stena quarry, the pelagic carbonate succes-

sion attains a thickness of about 250 m (Fig. 2). The Upper

Tithonian is represented by grey and subordinate red-brownish

thick bedded limestones. The uppermost 10 m of this succes-

sion are represented by marly limestones.

Microfacies analysis

Five microfacies were recognized: bioclastic wackestone

(MFT 1) is the dominant microfacies; subordinate are bio-

clastic‒peloidal wackestone (MFT 2), bioclastic‒peloidal

wacke stone / packstone (MFT 3), mudstone (MFT 4), and

brecciated bioclastic wackestone (MFT 5) (Figs. 3‒4).

Microfacies and biota indicate that the limestones deposited

in an open-shelf environment below the fair weather base.

Limestone consists of microfacies types that can be assigned

to the following Standard Microfacies (SMF) types after

Flügel (2010): SMF 3 — pelagic lime mudstone and wacke-

stone with pelagic microfossils, and SMF 4 — microbreccia,

bioclastic–lithoclastic packstone or rudstone.

Texture and composition of the carbonates are very similar

to those of the Rosomač Limestones in eastern Serbia pointing

to deposition under slope and toe-of-slope environments

(Petrova et al. 2012).

MFT 1 Bioclastic wackestone

The most frequent microfacies type in the limestones is

bioclastic wackestone, which was recorded throughout the

succession. The matrix is fine bioclastic micrite occasionally

crossed by sparry calcite-filled veins (Figs. 3/1–4; 4/1, 3, 6,

8–10). In the lower part of the succession bioclasts are rare

benthic foraminifera (Lenticulina sp.), juvenile ammonites,

recrystallized calcareous dinocysts, shell fragments and aptychi

(Fig. 3/1–4). Bioclastic wackestones observed in the upper

horizons contain calpionellids (Figs. 3/7, 10; 4/1, 9), rare intra-

clasts (Fig. 3/10), gastropods, shell fragments and calcareous

dinocysts (Fig. 4/6, 8, 10).

Rare skeletal debris from resedimented shallow-water

benthic foraminifera and gastropods mixed with finer pelagic

sediments was derived from platform-margin environments.

MFT 2 Bioclastic peloidal wackestone

These microfacies occurs as intercalations between the bio-

clastic wackestones. The main characteristic is the presence of

dispersed (Fig. 3/5) or densely packed peloids (Fig. 4/2, 4, 5) in

wackestone formed by debris flows in slope sequences. This

microfacies is characterized by the presence of skeletal grains

Fig. 1. Location of the Upper Tithonian section studied in Jelenska Stena quarry, Danube River Gorge, Carpatho‒Balkanides.

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Fig. 3. Thin-section photomicrographs

of the determined microfacies types

from the Upper Tithonian section in

Jelenska Stena quarry, showing cha-

rac

teristic component distributions

and fabrics. 1, 2 — bioclastic wacke-

stone with micritic matrix crossed by

sparry calcite-filled veins; filaments

and aptychi are present; low-diversity

benthic foraminifera association,

predominantly hyaline forms repre-

sented by Lenticulina sp., sample 21;

3, 4 — bioclastic wackestone with

micritic matrix crossed by subparallel

sparry calcite-filled veins; subordinate

recrystallized calcareous dinocysts

are present; juvenile ammonite

crossed by calcite-filled crack can be

seen, 3 ‒ sample 22, 4 ‒ sample 24;

5 — bioclastic–peloidal wackestone

with micritic matrix crossed by sparry

calcite-filled veins; dispersed peloids

in micritic matrix; skeletal grains are

predominately filaments, sample 27;

6 — bioclastic–peloidal wackestone/

packstone with micritic matrix crossed

by sparry calcite-filled veins; common

bioclasts are textulariids, filaments

and calcareous dinocysts, sample 29;

7 — bioclastic wackestone with

micritic matrix; longitudinal and

transversal sections of calpionellids

can be seen; calcareous dinocysts are

also present, sample 32; 8, 9 — mud-

stone with micritic and microspar

calcite matrix and calcareous dino-

cysts, 8 ‒ sample 36, 9 ‒ sample 37;

10 — bioclastic wackestone with micro-

spar matrix; intraclasts consis ting of

micrite associated with a gastropods

are common; longitudinal sections of

a high-spired gastropod and calpio-

nellids can be noticed; sample 38.

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CALPIONELLIDS OF THE UPPER TITHONIAN PELAGIC CARBONATES IN NORTHEASTERN SERBIA

GEOLOGICA CARPATHICA

, 2018, 69, 3, 301–311

Fig. 4. Thin-section photomicrographs

of the determined microfacies types

from the Upper Tithonian section in

Jelenska Stena quarry, showing cha-

racteristic component distributions

and fabrics. 1 — bioclastic wacke-

stone with micritic matrix crossed by

sparry calcite-filled veins; numerous

longitudinal and transversal sections

of calpionellids, sample 39; 2 — bio-

clastic–peloidal wackestone with

micritic matrix; peloids are densely

packed; subordinate intraclasts consist

of micrite and skeletal grains, sample

40; 3 — bioclastic wackestone with

micritic matrix crossed by sparry

calcite-filled veins; skeletal grains are

predominately calcareous dinocysts

and filaments, sample 42; 4, 5 ‒ bio-

clastic–peloidal wackestone with

micritic matrix; skeletal grains are

predominately calcareous dinocysts

and filaments; peloids are densely

packed; intraclasts consist of a micrite,

peloids and skeletal grains, sample 43;

6 — bioclastic wackestone with

micritic matrix crossed by sparry

calcite-filled veins; common bioclasts

are gastropods, filaments and calca-

reous dinocysts; longitudinal section

of a high-spired gastropod displaced

along sparry calcite-cement filled

microfractures, sample 44; 7 — brec-

ciated bioclastic wackestone with

mic ritic matrix crossed by sparry cal-

cite-filled veinlet, sample 46; 8 — bio-

clastic wackestone with micritic

matrix crossed by sparry calcite-filled

veinlet; common bioclasts are recrys-

tallized calcareous dinocysts, sample

47; 9, 10 — bioclastic wackestone

with micritic matrix crossed by sparry

calcite-filled veinlet; skeletal grains

are predominately calcareous dino-

cysts and calpionellids, 9 ‒ sample 49,

10 ‒ sample 50.

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predominately shell fragments (Fig. 3/5), but it also contains

intraclasts (Fig. 4/4, 5).

MFT 3 Bioclastic‒peloidal wackestone/packstone

Bioclastic–peloidal wackestone/packstone contains textu-

lariids, elongated shells and calcareous dinocysts in peloidal

micritic matrix (Fig. 3/6). Peloids are small and densely

packed. Veins are filled by calcite that is commonly sparry.

This microfacies is observed only in the lower part of the suc-

cession having a thickness of about 13 m.

MFT 4 Mudstone

Mudstone microfacies has been found in horizons about 5 m

thick intercalated between bioclastic wackestones in the mid-

dle part of the succession. Rare fragmented bioclasts occur in

a matrix of micrite and microspar (Fig. 3/8, 9).

MFT 5 Brecciated bioclastic wackestone

The microfacies has only been found in horizons about 5 m

thick near the top of the succession. Many bioclasts are hardly

recognizable in a strongly tectonized micritic matrix contai-

ning angular fragments crossed by sparry calcite-filled veinlet

(Fig. 4/7). The microfacies is interpreted as a debris-flow

deposit.

Microfossils and biostratigraphy

Biostratigraphic sequence A

Benthic foraminifera occur only in the lower part of the suc-

cession (Fig. 2). This sequence attains a thickness of about

65 m. It is represented by grey thick-bedded limestones

marked by rare occurrence of textulariids (Fig. 5/1) with

Textularia sp. cf. T. bettenstaedti (Fig. 5/2), associated with

Lenticulina sp. (Fig. 5/3), Everticyclammina praekelleri

(Fig. 5/4) and the encrusting organism Crescentiella morro

nensis (Fig. 5/5). A specimen of Tintinnopsella carpathica

(Fig. 6/1) has also been found in this sequence.

Benthic foraminifers

Although taxonomic diversity of benthic foraminifera is

low, they represent significant biostratigraphic markers useful

for palaeoenvironmental interpretation, too.

Everticyclammina praekelleri represents the most biostrati-

graphically important taxon for the lower part of succession.

It is typical for the Kimmeridgian‒Tithonian (Banner &

Highton 1990; Krajewski & Olszewska 2007; Olszewska et al.

2012; Pleş et al. 2015; Mircescu et al. 2016). The species is

a common internal-platform constituent, but has also been

recorded in carbonate margin deposits (Mircescu et al. 2016),

back-arc basins (Krajewski & Olszewska 2007), and pelagic

environments (Bubík & Reháková 2017), thus indicating

transport to deep-water settings.

Textularia sp. cf. T. bettenstaedti has longer stratigraphic

distribution from Berriasian to Aptian in the Northern Tethys

Margin (Salaj 1984; Gradstein et al. 1999), but it is also known

from the Upper Tithonian pelagic limestones of Stara Planina–

Poreč Zone in the trans-border area of eastern Serbia and

Bulgaria (Petrova et al. 2012).

Lenticulina sp. has a greater stratigraphic range, as it

occurs throughout the Jurassic and Cretaceous. It is common

in open-sea environments along the shelf-to-basin transition

(Hughes 2000; Reolid et al. 2008a, b).

Fig. 5. Thin-section photomicrographs of the determined benthic

foraminifera and microproblematica from the Upper Tithonian section

in Jelenska Stena quarry. 1 — textulariids; sample 25; 2 —

Textularia

sp. cf. T. bettenstaedti Bartenstein & Oertli;

sample 25; 3 — Lenticulina

sp.; sample 25; 4 — Everticyclammina praekelleri Banner & Highton;

sample 30; 5 — Crescentiella morronensis (Crescenti), sample 29.

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Incerate sedis

Crescentiella morronensis is associated with benthic fora-

minifers in the lower part of succession. This species is abun-

dant in Upper Jurassic and Lower Cretaceous platform and

slope deposits (Flügel 2010). Senowbari-Daryan et al. (2008)

considered Crescentiella morronensis as a symbiosis between

a nubeculariid foraminifera and calcifying cyanobacteria

common in open marine environments of the Tethyan Realm.

The significance of the C. morronensis is of less importance in

age determination as it ranges from the Upper Oxfordian to

the Aptian (Matyszkiewicz & Felisiak 1992; Senowbari-

Daryan et al. 2008; Schlagintweit 2012; Kaya & Altiner 2015).

However, the Kimmeridgian–Tithonian interval was a bloo-

ming period of the Crescentiella morronensis in the Tethyan

Realm (e.g. Pleş et al. 2017).

Age and correlations

The microfossil assemblage from the lower part of the suc-

cession indicates a Late Tithonian age. Of special stratigraphic

interest is the first occurrence of the calpionellid species

Tintinnopsella carpathica with a range from early Late

Tithonian through early Valanginian (Remane 1963, 1983).

Textularia sp. cf. T. bettenstaedti with a first appearance in

the Late Tithonian also worth mentioning. The age of the

sequence is also supported by the presence of Everticyclammina

praekelleri because its range does not extend into the Early

Berriasian. Crescentiella morronensis represents a very com-

mon microencruster species for the Upper Tithonian carbonate

deposits in the Getic carbonate platform and Southern

Carpathians (e.g., Bucur et al. 2010; Catincuţ et al. 2011;

Mircescu et al. 2016). We are thus assured of the Late Tithonian

age for the lower part of the succession.

Lenticulina sp. is recorded globally and Crescentiella

morronensis has a wide geographical distribution, as it is des-

cribed from many localities in the Tethyan Realm. Everti

cyclammina praekelleri has recently been recorded from

the northern Tethyan margins in the Getic carbonate platform

of the Romanian Southern Carpathians where it is reported for

the first time by Mircescu et al. (2016), and from southern

Poland (Olszewska et al. 2012). It was also documented from

other localities, including the southern Ukraine (Krajewski &

Olszewska 2007), and more recently from the Czech Republic

(Bubík & Reháková 2017), where it was recorded within

the Late Tithonian Crassicolaria Zone. Textularia sp. cf.

T. bettenstaedti was previously found in the trans-border area

of eastern Serbia and Bulgaria (Petrova et al. 2012).

Benthic foraminiferal and encrusting assemblages in north-

eastern Serbia are most similar to those from Romania and

border area of eastern Serbia and Bulgaria.

Biostratigraphic sequence B

The calpionellids become totally dominant from 65 to

105 m above the base of the succession through a thickness of

about 40 m. The calpionellid-bearing sequence is marked by

the first occurence of calpionellid association in the sample 31.

It is represented by grey thick-bedded limestones with calpio-

nellid association dominated by crassicollarians accompanied

by genus Calpionella.

Calpionellids

The calpionellid species belong to the Crassicollaria

Standard Zone. This association is characterized by the explo-

sion in variety of species. The crassicolarian association is

diverse and represented by Crassicollaria brevis (Fig. 6/3),

Fig. 7. Thin-section photomicrographs of the determined calpionellids from the Upper Tithonian section in Jelenska Stena quarry.

1–5 — Crassicollaria intermedia (Durand-Delga); 1 ‒ sample 31, 2–3 ‒ sample 32, 4 ‒ sample 38; 5 ‒ sample 50. 6-8 ‒ Crassicollaria sp.;

6 ‒ sample 33, 7–8 ‒ sample 38. Scale bar = 100 μm.

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Crassicollaria parvula (Fig. 6/6–7), Crassicollaria massu

tiniana (Fig. 6/8–11), Crassicollaria sp. (Fig. 7/6–8), and

Crassicollaria intermedia (Figs. 6/24, 7/1–4). Calpionella sp.

(Fig. 6/4–5) and Calpionella alpina (Fig. 6/12–23) are common.

The sequence also includes rare Tintinnopsella carpathica

(Fig. 6/2). All taxa disappeared in the uppermost part of

the sequence apart from Crassicollaria intermedia.

All calpionellid species are widely known worldwide

from the Upper Tithonian and reveal a strong similarity to

the Tethyan Realm.

Age and correlations

Crassicollaria intermedia and Crassicollaria massutiniana

are very good age markers, being confined to the early Late

Tithonian (Remane 1983). These species clearly indicate

the presence of Upper Tithonian calpionellid associations just

below the Jurassic/Cretaceous boundary.

The calpionellid association marked by maximum diversi-

fication of the genus Crassicollaria is referred to the Crassi

colaria Zone, Intermedia Subzone in Olóriz et al. (1995),

Pop (1997), Andreini et al. (2007), Grabowski et al. (2010).

The association also refers to Crassicolaria Zone, Massu

tiniana Subzone in the Western Balkanides (Lakova et al.

1999; Petrova et al. 2012; Lakova & Petrova 2013), or Brevis

Subzone (sensu Reháková & Michalík 1997).

The Upper Jurassic sequence may be also compared to other

well-documented sites in adjacent regions of Romania and

Bulgaria. The biostratigraphic sequence B corresponds in

general lithologic character and calpionellid association to

the Upper Tithonian Marila limestones of the Reşita–Moldova–

Nouă zone north of Danube in the Romanian Southern

Carpathians (Pop 1997; Bucur 1997). Towards the Serbian–

Bulgarian border in the east, the calpionellid-bearing sequence

can be compared to the Massutiniana Subzone (Crassicolaria

Zone) of the Rosomač Limestones in the Stara Planina‒Poreč

Zone and the Glozhene limestone formation in the West

Balkan (Lakova et al. 1999; Petrova et al. 2012).

Biostratigraphic sequence C

In the overlying uppermost part of the succession calpionellids

are very rare. The thickness of the sequence C reaches about

145 m. It was only possible to recognize Crassicollaria inter

media (Fig. 7/5) in the topmost parts of the succession repre-

sented by marly limestones through a thickness of about 13 m.

According to the occurrence of isolated Crassicollaria inter

media, the biostratigraphic sequence C should have been

deposited in the Late Tithonian, too. The whole succession

from base to top is therefore certainly of Late Tithonian age.

Conclusion

The present study documents an Upper Tithonian carbonate

succession in NE Serbia deposited in a deep shelf margin

along the northern margin of the Alpine Tethys Ocean. Slope

and toe-of-slope environments prevailed in the study area.

The depositional setting of carbonate succession corresponds

to the standard facies zones 3 and 4 by Flügel (2010).

The microfossil assemblage although not rich in number of

species represents the first records of Late Tithonian pelagic

microfossil biota from the further north Getic of the Serbian

Carpatho‒Balkanides and, therefore, expands the current

knowledge on their palaeogeographical distribution.

Recognized benthic foraminifers represent cosmopolitan

taxa in the northern Tethyan Realm shelves during the Late

Tithonian. Benthic foraminiferal associations in northeastern

Serbia are similar to those from adjacent regions of Romania

and Bulgaria. The majority of calpionellid taxa correspond to

the widely known Crassicollaria Zone. Scarcity of some

important stratigraphic markers prevents precise establish-

ment of subzones.

The Tithonian–Berriasian boundary was not documented

because stratigraphic succession lacks the topmost calpio-

nellid-bearing intervals with important stratigraphic markers

due to complicated tectonic framework in the further Getic of

northeastern Serbian Carpatho‒Balkanides.

Acknowledgements: We are grateful to Prof. Daniela

Reháková (Comenius University, Bratislava), Dr. Jozef

Michalík (Slovak Academy of Sciences, Bratislava) and

Dr. Kamel Maalaoui (Faculty of Sciences and Geolocical

Survey, Tunis) for their helpful comments on the calpionellids.

Two anonymous reviewers are thanked for valuable correc-

tions and helpful comments that helped to improve the origi-

nal manuscript. Heather Hobson (Manchester, England) is

thanked for the English corrections. This work was supported

by the Ministry of Education, Science and Technologi cal

Development of the Republic of Serbia, Project No. 176017.

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Appendix

List of microfossils recognized in this study, arranged in alphabetical order. Taxa are illustrated in Figs. 5–7.

a) Calpionellids

Tintinnopsella carpathica (Murgeanu & Filipescu)

Crassicollaria brevis Remane

Crassicollaria intermedia (Durand-Delga)

Crassicollaria massutiniana (Colom)

Crassicollaria parvula Remane

Crassicollaria sp.

Calpionella alpina Lorenz

Calpionella sp.

b) Benthic foraminifera

Textulariids

Textularia sp. cf. T. bettenstaedti Bartenstein & Oertli

Lenticulina sp.

Everticyclammina praekelleri Banner & Highton

c) Incertae sedis

Crescentiella morronensis (Crescenti)