ORIGINAL ARTICLE

Encrusting micro-organisms and microbial structures in UpperJurassic limestones from the Southern Carpathians (Romania)

George Ples • Cristian V. Mircescu •

Ioan I. Bucur • Emanoil Sasaran

Received: 16 July 2012 / Accepted: 18 July 2012 / Published online: 1 September 2012

� Springer-Verlag 2012

Abstract Late Jurassic–Early Cretaceous Stramberk-type

reef limestones are known from some parts of the Southern

Carpathians in Romania. The Upper Jurassic deposits

mainly consist of massif reef limestones including a variety

of microbialites associated with micro-encrusters. They

played an important role in the formation and evolution of

the reef frameworks and thus are of significant importance

for deciphering the depositional environments. For our

study, the most important encrusting organisms are Cres-

centiella morronensis, Koskinobullina socialis, Lithocodi-

um aggregatum, Bacinella-type structures, Radiomura

cautica, Perturbatacrusta leini, Coscinophragma sp., and

crust-forming coralline sponges such as Calcistella. Based

on microscopic observations, microbial contribution to reef

construction is documented by the abundance of dense

micrite, laminate structures, clotted, thrombolithic or

peloidal microfabrics, constructive micritic cortices,

biogenic encrustations and cement crusts, as well as by other

types of microbial structures and crusts. Most of the

investigated carbonate deposits can be classified as

‘‘coral-microbial-microencruster boundstones’’ which are

characteristic for the Intra-Tethyan domain. Their paleo-

geographical significance is indicated by the presence of

many features comparable with carbonate deposits of

rimmed platform systems from the Northern Calcareous

Alps or Central Apennines. Based on the distribution of the

facies and facies associations within the carbonate sequen-

ces under study we can distinguish slope and external shelf

margin environments. The microbial crusts, the encrusting

micro-organisms, and in some cases the syndepositional

cements have stabilized and bound the carbonates of the slope

facies types. Subsequently, the stable substrate favored the

installation of coral-microbial bioconstruction levels.

Keywords Microfacies � Micro-encrusters � Microbial

structures � Upper Jurassic � Southern Carpathians �Romania

Introduction

The present study focuses on the importance of micro-

encrusters and microbial structures in the formation and

stabilization of the Upper Jurassic reefs in Romania. We

compared two distinctive sections in areas characterized by

similar geological histories: Buila–Vanturarita and Piatra

Craiului massifs. Both areas, together with other areas in

the Southern Carpathians where Mesozoic deposits crop

out, constitute the sedimentary cover of the Getic Nappe.

Most of the carbonate deposits in the area under study

consist of coral-microbial facies types including diverse

encrusting organisms. The Buila–Vanturarita Massif is

represented by a NE–SW trending calcareous ridge located

in the central-southern part of the Southern Carpathians. It

mainly consists of Upper Jurassic deposits. The Piatra

Craiului Massif is represented by a prominent ridge located

at the eastern end of the Southern Carpathians; it also

consists of carbonate deposits that crop out on both flanks

of the ridge. Our study is based on the thin-section

G. Ples (&) � C. V. Mircescu � I. I. Bucur � E. Sasaran

Department of Geology, Babes-Bolyai University,

M. Kogalniceanu 1, 400084 Cluj-Napoca, Romania

e-mail: george.ples@ubbcluj.ro

C. V. Mircescu

e-mail: mircescu_cristian2005@yahoo.com

I. I. Bucur

e-mail: ioan.bucur@ubbcluj.ro

E. Sasaran

e-mail: emanoil.sasaran@ubbcluj.ro

123

Facies (2013) 59:19–48

DOI 10.1007/s10347-012-0325-1

investigation and illustration of the encrusting organisms

and microbial structures identified in the two areas

with special emphasis on paleoenvironments and their

interpretation.

Geological background

The carbonate deposits cropping out in the Buila–Vantu-

rarita and Piatra Craiului calcareous massifs are included in

Fig. 1 Geological map of Buila-Vanturarita Massif (modified after

Lupu et al. 1978). 1 Magmatic rocks. 2 Sebes-Lotru metamorphic

series. 3 Cozia metamorphic series. 4, 5 Triassic. 6 Bajocian-

Callovian. 7 Callovian-Oxfordian. 8 Kimmeridgian-Tithonian. 9

Barremian-Aptian. 10 Albian-Cenomanian. 11 Coniacian-Santonian.

12 Campanian–Maastrichtian. 13 Ypresian-Lutetian. 14 Lutetian-

Priabonian. 15 Oligocene. 16, 17 Lower Miocene. 18 Middle

Miocene. 19, 20 Upper Miocene. 21–23 Quaternary deposits

20 Facies (2013) 59:19–48

123

the sedimentary cover of the Getic Nappe, a structural unit

of the Median Dacides of the Southern Carpathians

(Sandulescu 1984).

Buila-Vanturarita Massif

The Buila-Vanturarita Massif is located in the central

south-western part of the Southern Carpathians. It repre-

sents the only calcareous block in the Capatanii Mountains,

and it consists of a NE–SW-oriented ridge (Fig. 1). The

Jurassic deposits are abundant, being represented by

detrital silty and siliceous Middle Jurassic rocks overlain

by Upper Jurassic (Oxfordian to Tithonian) reef carbonates

(Dragastan 2010). Boldor et al. (1970) defined the fol-

lowing lithological succession for the Middle Jurassic:

micaceous calcareous sandstones and marls (Upper

Bathonian–Lower Callovian), followed by marly lime-

stones and limestones (Middle and Upper Callovian). The

authors based their age assignment on some specimens

of Phylloceras sp. and Bositra buchi Roemer. The

Fig. 2 Geological map of Piatra Craiului Massif (modified after

Dimitrescu et al. 1971, 1974; Patrulius et al. 1971; Sandulescu et al.

1972). 1 Cumpana metamorphic series. 2 Leaota metamorphic series.

3 Magmatic rocks. 4 Bajocian-Callovian. 5 Callovian-Oxfordian. 6

Kimmeridgian-Berriasian-?Lower Valanginian. 7 Hauterivian. 8Barremian. 9 Aptian. 10 Albian. 11 Vraconian-Cenomanian. 12Turonian-Maastrichtian. 13 Paleogene. 14–17 Quaternary deposits

Facies (2013) 59:19–48 21

123

Kimmeridgian–Tithonian interval is best represented in the

succession of the Buila-Vanturarita Massif; the corre-

sponding deposits are massive reef limestones, locally

reaching several hundred meters in thickness (Dragastan

2010).

Lower Cretaceous (Berriasian–Valanginian and Barre-

mian–Aptian) deposits are known from isolated, small

areas north of Arnota Peak, Costesti Gorges, and Cacova.

They are located on the top of the massive Upper Jurassic

limestones. In these Lower Cretaceous deposits, Dragastan

(1980, 2010) had identified a micropaleontological asso-

ciation with Trocholina alpina Leupold, Macroporella

praturloni Dragastan, Salpingoporella annulata Carozzi,

Actinoporella podolica Alth, Montsalevia salevensis Cha-

rollais, Bronnimann and Zaninetti, Melathrokerion sp.,

Cayeuxia moldavica Frollo, and Felixporidium atanasiui

Dragastan, corresponding to the Berriasian–Valanginian

interval. However, Uta and Bucur (2003) described several

microfossils (Vercorsella hensoni Dalbiez, Vercorsella cf.

camposaurii Sartoni & Crescenti, Charentia sp., Everticy-

clammina sp, and Falsolikanella danilovae Radoicic) that

indicate a Barremian-Lower Aptian age.

The Upper Cretaceous sedimentary deposits are mainly

detrital, consisting of sandstones and conglomerates; they

are located in the eastern and north–eastern part of the

massif. Three major complexes were separated: a lower

Cenomanian–Turonian complex, a middle Coniacian–

Santonian complex, and an upper Campanian–Maastrich-

tian complex (i.e., Brezoi Formation) (Boldor et al. 1970;

Todirita-Mihailescu 1973).

Piatra Craiului Massif

In this area, a succession of Jurassic and Cretaceous sedi-

ments consisting of sandstones, marls and limestones with

diverse lithologies and fossiliferous associations overlays

the crystalline basement assigned to the Cumpana and

Leaota series (Popescu 1966). They form a N–S-oriented

syncline in the central-western part of the sedimentary

area, known in the literature as the Dambovicioara Couloir

(Patrulius 1969) (Fig. 2). At the base of the succession,

microconglomerates, sandstones, and marly limestones

gradually pass into marly limestones and radiolarites

Fig. 3 Location of the sampled sections. a Bistrita Gorges section

(Buila-Vanturarita). 1, 2 Metamorphic rocks. 3 Kimmeridgian-Titho-

nian limestones. 4–8 Miocene deposits. 9–11 Quaternary deposits. 12Faults. 13 Studied section (P1). b Vladusca Valley section (Piatra

Craiului). 1 Metamorphic rocks. 2 Bajocian–Lower Callovian lime-

stones. 3 Upper Callovian–Oxfordian limestones. 4 Kimmeridgian–

?Lower Valanginian limestones. 5–7 Quaternary deposits. 8 Faults. 9Studied section (P2)

Fig. 4 Field pictures. a View of the southern entrance in Bistrita

Gorges (southeastern part of the Buila-Vanturarita Massif). b Massive

reefal limestone succession from Bistrita Gorges. c Large limestone

blocks in the Bistrita Gorges. d Panoramic view of the limestones

which outcrop in the western part of Piatra Craiului Massif. e Banks

of Stramberk-type limestones from Vladusca Valley, Piatra Craiului

Massif. f Massive limestones of the Stramberk-type succession in

Piatra Craiului Massif. g Coral boundstone with branching corals

(Vladusca Valley, Piatra Craiului Massif)

c

22 Facies (2013) 59:19–48

123

Facies (2013) 59:19–48 23

123

(Popescu 1966). Based on the identified fragments of

Posidonia (=Bositra) buchi Roemer and ammonites (Peri-

sphinctidae), Popescu (1966) assigned the lowermost

deposits to the Bajocian–Lower Callovian, in agreement

with Jekelius (1938) and Oncescu (1943). Additionally,

Popescu (1966) has assigned the radiolarites to the Middle

Callovian–Oxfordian without any paleontological evi-

dence. The age was proposed based on similarities with

other deposits in the western flank of the Bucegi Massif

(Patrulius 1957). Bucur (1980), Meszaros and Bucur

(1980) and Beccaro and Lazar (2007) studied sponges,

nannoplankton, and radiolarians on the Bajocian–Oxfor-

dian deposits from Piatra Craiului and provided arguments

for the Oxfordian age of the radiolarites.

The Kimmeridgian–Tithonian deposits consist of

massive or stratified limestones; the latter form decimeter-

thick beds. Bucur (1978) assigned a Kimmeridgian–

Tithonian age to the lower part of the white massive

limestones based on a micropaleontological association

with Sacoccoma sp., Cadosina fusca Wanner, Cladocor-

opsis mirabilis Felix, Bacinella irregularis Radoicic, and

Spirillina sp. From the top of the succession, Bucur

(1978) described a microfossil association typical for the

Berriasian–?Lower Valanginian interval (T. alpina Leu-

pold, Everticyclamina virguliana Koechlin, C. moldavica

Frollo, Acicularia elongata Carozzi). In a more recent

paper, Bucur et al. (2009) provided new data on the

micropaleontological content of these limestones by

describing an association consisting of calcareous algae

(Campbeliella striata Carozzi, Clypeina sulcata Alth, C.

parasolkani Farinacci and Radoicic, S. annulata Carozzi,

Salpingoporella pygmaea Gumbel, Selliporella neocomi-

ensis Radoicic), foraminifera (Andersenolina alpina

Leupold, Mohlerina basiliensis Mohler, Protopeneroplis

striata Weynschenk, P. ultragranulata Gorbachik,

Anchispirocyclina lusitanica Egger, Coscinophragma sp.,

Charentia sp., Lenticulina sp.), and encrusting organisms

(bacinellid-structures, Crescentiella morronensis Cres-

centi, L. aggregatum Elliott, Mercierella dacica Draga-

stan, and R. cautica Senowbari-Daryan & Schafer).

Among these forms, Clypeina parasolkani, S. neocomi-

ensis, and Protopeneroplis ultragranulata are character-

istic of the Berriasian–?Lower Valanginian and thus

document the continuation of the carbonate sedimentation

during the Berriasian and possibly the Lower Valanginian

in the western part of the Piatra Craiului Massif.

The central part of the Piatra Craiului syncline is rep-

resented by Aptian–Albian conglomerates dominantly

consisting of carbonate pebbles, and Vraconian–Cenoma-

nian polymictic conglomerates with carbonate and meta-

morphic clasts embedded in a siliciclastic matrix (Popescu

1966).

Sampled sections and methods

Our study is based on the investigation of 450 samples

collected from two distinctive sections (Figs. 3, 4): Cheile

Bistritei (Bistritei Gorges) (P1, Fig. 4a), located at the

south-western end of the Buila–Vanturarita crest, and a

section upstream in the Vladusca Valley (P2, Fig. 4b)

located in the central-western part of Piatra Craiului Mas-

sif. Sampling was performed at 6–7-m intervals in section

P1 and at 2–3-m intervals in section P2, respectively. Some

of the samples were cut longitudinally and polished to

allow evaluation of microfacies and fossil content. Detailed

investigation of microfacies types and micropaleontologi-

cal content was made using 410 thin-sections, of which 240

are from the Cheile Bistritei section (Buila–Vanturarita)

and 170 from the Vladusca section (Piatra Craiului).

Microphotographs were taken by using a Cannon Power-

shot A640 digital camera attached to a Zeiss Axioscope

microscope. The abundance charts were obtained with the

PAST (Palaeontological Statistics) software version 2.13

(Hammer et al. 2001).

Microfacies analysis

Cheile Bistritei section (Buila–Vanturarita Massif) (P1)

The sedimentary succession of Cheile Bistritei is com-

posed of thick units of reef carbonate breccia/microbreccia

interlayered with levels of coral-microbial bioconstructions

(Fig. 3). Packstone and grainstone occur subordinately (P1

in Fig. 5). Within these carbonate units we have identified

two main facies types: F1—intraclastic bioclastic rudstone/

grainstone and F2—Coral microbial boundstone, corre-

sponding to SMF 6 and SMF 7, respectively, of the stan-

dard microfacies types (Flugel 2004).

The dominant breccia/microbreccia levels show tabular

and layered geometries. The microfacies types are repre-

sented by intraclastic-bioclastic rudstone and intraclastic-

bioclastic coarse grainstone (F1). These consist mainly of

fragments of reef rocks represented by corals, sponges,

bryozoans, and intraclasts of coral-microbial boundstones,

stromatolitic-thrombolytic microbial crusts, or bioclastic

packstone with C. morronensis. As a rule, the reef-rock

fragments are angular to subangular in shape, while their

sizes range from millimeters to centimeters. The deposits

are poorly sorted, with chaotic arrangement of the clasts.

The matrix consists of carbonate bioclasts and intraclasts of

different sizes. Both in the matrix and in the clasts we have

identified a micropaleontological association consisting of

foraminifera (Protopeneroplis ultragranulata Gorbachik,

Protopeneroplis sp., Charentia evoluta Gorbachik, Lituola

24 Facies (2013) 59:19–48

123

Fig. 5 Succession of the limestone deposits from the Bistrita Gorges,

Buila-Vanturarita Massif (P1) and Vladusca Valley, Piatra Craiului

Massif (P2). 1 Coral-microbial boundstone. 2 Reefal microbreccia. 3

Corals. 4 Gastropods. 5 Echinoderms. 6 Peloids. 7 Bryozoans. 8Bivalves. 9 Dasycladalean algae. 10 Microbial crusts

Facies (2013) 59:19–48 25

123

26 Facies (2013) 59:19–48

123

baculiformis Schlagintweit & Gawlick, M. basiliensis

Mohler, A. alpina Leupold, Troglotella incrustans Wernli

& Fookes, Bullopora aff. laevis Sollas, Lenticulina sp.,

Coscinophragma sp., Ammobaculites sp.), calcareous algae

(C. sulcata Alth, S. pygmaea Gumbel, Thaumatoporella

parvovesiculifera Raineri, Nipponophycus ramosus Yabe

& Toyama, ‘‘Solenopora’’ sp.), calcified sponges (Murania

reitneri Schlagintweit, Neuropora lusitanica Termier,

Thalamopora lusitanica Termier and Termier, Calcistella

cf. jachenhausenensis Reitner), gastropods, bivalves, bry-

ozoans, and worm tubes.

The coral-microbial bioconstructions are interlayered in

the middle and upper parts of the succession, on top of the

intraclastic-bioclastic rudstone/grainstone facies (P1 in

Fig. 5). The following microfacies sub-types of F2 could

be identified: microbial bindstone, framestone, and spo-

radically bafflestone. The bioconstructions consist of corals

(Figs. 6c, 7c, f), sponges (Fig. 7a, g), bryozoans, and mi-

crobialites (Figs. 6d, 7b–d). The corals and sclerosponges

are intensely encrusted by algae (T. parvovesiculifera

Raineri), some microproblematic organisms (C. morron-

ensis Crescenti, R. cautica Senowbari-Daryan and Schafer,

P. leini Schlagintweit and Gawlick, K. socialis Cherchi and

Schroeder, L. aggregatum Elliott or bacinellid structures),

bryozoans, and encrusting foraminifera (Fig. 7). Within the

bioconstructions, the microbialites contain embedded reef

constituents such as corals and sponges which colonized

the intra-reef sediment (Figs. 6c, d, 7b, g). For the evalu-

ation of microbialites, we have used the classifications of

Riding (1991, 2000), Schmid (1996), and the discussion on

thrombolites in Shapiro (2000). The microbialites identi-

fied at the outer parts of the reef constituents are of the

stromatolitic and thrombolytic type. Besides peloids, also

silt-sized bioclasts and carbonate intraclasts occur agglu-

tinated in the stromatolitic crusts. The laminated meso-

structures mainly consist of micritic, grumelous and

laminated microstructures (Fig. 8a–d). The mesoglome-

rules, as main components of the clotted mesostructures,

display spherical shapes; they consist of a wide diversity of

peloids (Fig. 8b) and grumelous fabrics (Fig. 8c, d).

Microbialites are common components of the internal

sediment within the bioconstructions, being associated with

sponges, bryozoans, cyanobacteria, and some micropro-

blematic organisms (C. morronensis Crescenti, R. cautica

Senowbari-Daryan and Schafer). Syndepositional (radiax-

ial-fibrous) cement also played an important role in the

consolidation of the reef framework (Bathurst 1971, 1986;

Kendall and Tucker 1973; Kendall 1977; Saller 1986;

Flugel and Koch 1995). The content is often associated

with the microbialites (Fig. 7e).The internal sediment of

the bioconstructions is represented by peloidal wackestone/

packstone with C. morronensis Crescenti, microbialithic

bioclastic packstone and intraclastic bioclastic grainstone.

Table 1 Main microfossils

identified in the studied

successions and their

stratigraphic range

Fig. 6 Microfacies characteristics and encrusting organisms in the

limestones of the Buila-Vanturarita and Piatra Craiului Massifs.

a Intraclastic-bioclastic rudstone; Bistrita Gorges, Buila-Vanturarita

Massif, sample 191. b Bioclastic rudstone microfacies with coral and

echinoid fragments, and microbial structures; Bistrita Gorges, Buila-

Vanturarita Massif, sample P45. c Coral-microbial boundstone

associated with dense microbial crusts supporting the bioconstruction

framework; Bistrita Gorges, Buila-Vanturarita Massif, sample 106.

d Micro-encruster bindstone with Perturbatacrusta leini (P), Litho-codium aggregatum (L) and Crescentiella morronensis (arrow);

Bistrita Gorges, Buila-Vanturarita Massif, sample P29. e, f Coral

microbial bioconstructions; branching corals in transverse or longi-

tudinal section form the reefal framework. The sediment in between

corals consists of peloidal bioclastic thrombolytic/packstone. The

most common bioclasts are represented by encrusting organisms (e.g.,

Crescentiella morronensis) and encrusting foraminifera; e sample 9;

f sample 79, Vladusca Valley, Piatra Craiului Massif. g, h Bioclastic

intraclastic rudstone. Echinid fragments with syntaxial overgrowth

cement (arrow), coral fragments, and reworked encrusting organisms

are most common. Angular intraclasts of peloidal sediment are also

present; g sample 69; h sample 158, Vladusca Valley, Piatra Craiului

Massif. Scale bar is 1 mm

b

Facies (2013) 59:19–48 27

123

28 Facies (2013) 59:19–48

123

In addition, sponges, ?udoteacean algae (N. ramosus Yabe

and Toyama), microproblematic organisms (C. morronen-

sis Crescenti, R. cautica Senowbari-Daryan and Schafer,

Perturbatacrusta leini Schlagintweit and Gawlick),

foraminifera, dasycladalean algae, cyanobacteria, frag-

ments of mollusks, echinids, bryozoans, and worm tubes

(Terebella sp., Mercierella dacica Dragastan) are present

in the rock.

Vladusca section (Piatra Craiului Massif) (P2)

This section corresponds to the lower and middle part of

the white limestone succession from the Piatra Craiului

Massif. As in the case of the previously investigated

section, we have identified two main facies associations:

F1—intraclastic bioclastic rudstone and F2—coral micro-

bial boundstone, represented by reef breccia/microbreccia

and coral-microbial bioconstructions (P2 in Fig. 5).

The microbreccia levels (F1) are meter-thick and are

invariably present within the succession. The identified

microfacies are intraclastic-bioclastic rudstone and bio-

clastic rudstone/grainstone. These deposits are poorly sor-

ted and contain angular clasts represented by bioclasts

(echinoderm, coral, and gastropod fragments) and coral-

microbial crusts. Their shape and composition point to

limited transport in a reef slope environment (Fig. 6g, h).

In this succession, the bioconstructions (F2) consist of

bafflestone with peloidal wackestone as internal sediment,

framestone with wackestone/packstone as internal sediment,

and bindstone with encrusting organisms (Fig. 6e, f). These

facies alternate in the lower part of the succession. The

internal sediment of the boundstones consists of peloidal

wackestone with microbial crusts; the latter played a signif-

icant role in the stabilization of the reef bioconstructions.

We have identified bindstones with Bacinella-Lithocodium-

type structures (Fig. 9a, b), as well as framestones with

peloidal-bioclastic wackestone and common specimens of

C. morronensis Crescenti as internal sediment. Radiomura

cautica Senowbari-Daryan & Schafer and P. leini Schla-

gintweit & Gawlick occur only in the framestone levels,

accompanied by Coscinophragma sp., K. socialis Cherchi

and Schroeder, and Calcistella jachenhausenensis Reitner.

Also present are fragments of echinoderms, ammonite

‘‘nuclei’’, worm tubes and foraminifera (Protopeneroplis sp.,

C. evoluta Gorbachik, Lenticulina sp., and L. baculiformis

Schlagintweit and Gawlick). The middle part of the succes-

sion consists mainly of intraclastic-bioclastic rudstone. Bio-

constructions are subordinate, developed on the top of the

reef breccia/microbreccia. The main bioclasts types are rep-

resented by bryozoans, coral fragments, and microbial crusts.

Encrusting organisms are rare, and they are basically repre-

sented by bacinellid-type structures, L. aggregatum Elliott,

and C. morronensis Crescenti. Also present are rare frag-

ments of P. leini Schlagintweit and Gawlick. The angular-

subangular intraclasts consist of peloids bound by a micritic

matrix. Towards the top of the section, coral-microbial bio-

constructions (Fig. 9e, g) become preeminent; they are

interlayered with thin levels of peloidal bioclastic rudstone.

Crescentiella morronensis Crescenti, the bacinellid-type

structures and, L. aggregatum Elliott are present in ratios

similar to those evaluated in the lower part of the section.

Significant concentrations of P. leini Schlagintweit & Gaw-

lick and R. cautica Senowbari-Daryan & Schafer are also

present (Fig. 9f). Stromatolitic structures with micritic or

peloidal microstructures developed around the various bio-

clasts such as sclerosponges or corals. Radiaxial-fibrous,

botryoidal and blocky cements are the most common cement

types found in these deposits.

Facies interpretation

Similar facies and depositional environments were

noticed in the studied successions. Based on composition,

grain size, and shape of the carbonate rocks fragments, we

assign the reefal microbreccia deposits to gravitational

flows (Hopkins 1977; Enos and Moore 1983; Coniglio and

Dix 1992; Stow 1995; Einsele 1991). The facies types

point to a shelf slope environment; their horizontal and

vertical distribution are typical for the margins of a car-

bonate platform. The association of the intra-reef sedi-

ment and the microbial encrustations point to low

sedimentary rates that favored the initiation and the

development of bioconstructions. Based on the composi-

tion and the textural-structural features, we have assigned

the facies associations above to the median-proximal

areas on the shelf-crest of a reef-slope environment

(McIlreath and James 1984; Grammer et al. 1991;

Fig. 7 Microencrusters and frame builders in the carbonate succes-

sion of the Buila-Vanturarita Massif. a Large sclerosponge crust

(arrow) with Calcistella jachenhausenensis (Cj) and other encrusters

such as Crescentiella morronensis (C), Lithocodium aggregatum (L),

and serpulid worm tubes (S), in a coral boundstone/framestone.

b Dense microencruster framework; Crescentiella morronensis spec-

imens are present within the crust (arrow). c Microencruster aglo-

merae covering a stromatolitic/thrombolytic structure followed by a

bindstone-type microfacies. d Bacinellid meshwork (B) between

corals. e Growth cavity filled with radiaxial-fibrous cement (arrows).

f Gastrochaenolites boring with geopetal fill (arrow) in a branching

coral. g Large specimen of Neuropora lusitanica (N), a very common

taxon within the samples; Salpingoporella pygmaea (arrow) is also

visible in the middle part of the picture. h Nipponophycus ramosus(arrows) boundstone. a–h, Bistrita Gorges, Buila-Vanturarita Massif;

a sample 148; b sample 112; c sample 197; d sample P41; e sample

199; f sample 165; g sample 145; h sample 164. Scale bar is 1 mm

b

Facies (2013) 59:19–48 29

123

Ginsburg et al. 1991). This assignment is also supported

by the association with bioconstructions. The abundance

of gravitational flows in the succession attests to an outer

shelf-margin paleoslope.

Associated biota and age of the limestones

The most important microfossils (foraminifera and calcar-

eous algae), encrusting organisms and calcareous sponges/

sclerosponges are listed in Table 1. The micropaleonto-

logical assemblage with C. sulcata, S. pygmaea, N. ramo-

sus, C. evoluta, A. alpina, together with the sponge

assemblage, indicates a Late Jurassic age (Bucur 1999;

Schlagintweit et al. 2005). Moreover, in the Piatra Craiului

Massif, the index microfossils for the Berriasian (and

possibly the Lower Valanginian) e.g., M. salevensis and

S. neocomiensis (Bucur et al. 2009) occur at levels above

the deposits under study. This represents an additional

argument for the Kimmeridgian–Tithonian age of the

studied carbonate levels. Similar associations have been

described by Dragastan (1975), Bucur and Sasaran (2005),

Sasaran (2006) and Bucur et al. (2010) in other Kimme-

ridgian–Tithonian deposits in Romania.

Encrusting organisms and microbial crusts

The associations of encrusting organisms identified in the

two studied sections are taxonomically diverse; the most

common and significant taxa are discussed below.

Crescentiella morronensis Crescenti 1969 (= ‘‘Tubi-

phytes’’ morronensis Crescenti auct.) Fig. 10a–d

Crescenti (1969) considered Tubiphytes morronensis as

an encrusting organism built-up of micritic cylindrical

Table 2 Crescentiella morronensis occurrences within the Tethyan domain

Author Zone Age Country

Radoicic (2005) Mirdita region Lower Valanginian Albania

Schlagintweit and Gawlick (2008),

Gawlick et al. (2009)

Plassen carbonate platform,

Northern Calcareous Alps

Upper Tithonian–Lower Berriasian Austria

Eliasova (1981) Stramberk Tithonian Czech

Republic

Pomoni-Papaioannou et al. (1989) Western Molasse basin Upper Jurassic Germany

Keupp et al. (1993), Flugel (1981) Southern Frankenalb Upper Jurassic

Carras and Georgala (1998) Chalikidiki Peninsula Upper Jurassic–Lower Cretaceous Greece

Senowbari-Daryan et al. (2008) Madonie Mountains, Sicily Tithonian Italy

Matyszkiewicz and Felisiak

(1992)

Cracow Upland, Polish Jura Chain Upper Oxfordian Poland

Bucur et al. (2005) Outer Carpathians and Holly Cross Mountains Upper Oxfordian–Lower

Kimmeridgian

Hoffmann et al. (1997) Holly Cross Mountains Oxfordian–Kimmeridgian

Schmid (1995) Lusitanian Basin Kimmeridgian Portugal

Dragastan (1969) Bicaz area, Eastern Carpathians Upper Jurassic Romania

Uta and Bucur (2003) Buila-Vanturarita Massif, Southern

Carpathians

Kimmeridgian–Tithonian

Serban et al (2004) Caprioara-Pojoga area, Mures Trough Kimmeridgian–Tithonian

Sasaran et al. (2000, 2001),

Sasaran (2006)

Trascau Mountains Upper Jurassic–Lower Cretaceous

Reolid et al. (2005),

Reolid and Gaillard (2007)

Prebetic zone, Betic Cordillera Kimmeridgian–Tithonian Spain

Fig. 8 Microbial structures of the reef limestones from the Buila-

Vanturarita and Piatra Craiului massifs. a Agglutinated stromatolitic/

peloidal mesostructure; Bistrita Gorges, Buila-Vanturarita Massif,

sample P55a. b Peloidal stromatolite; Bistrita Gorges, Buila-Vantu-

rarita Massif, sample 155. c, d Clotted mesostructure displaying

grumelous features; also note the serpulid tubes in c (S); Bistrita

Gorges, Buila-Vanturarita Massif, sample 166. e Clotted microbial

crusts associated with C. jachenhausenensis (Cj) and Crescentiella(C) type structures; Vladusca Valley, Piatra Craiului Massif, sample

31. f Gradual transition from stromatolitic fabric to clotted/grumelous

fabrics; Vladusca Valley, Piatra Craiului Massif, sample 92.

g Calcareous sponge encrusted by microbial structures developing

grumelous fabrics; noticed platy microsolenid below; Vladusca

Valley, Piatra Craiului Massif; sample 122. Vladusca Valley, Piatra

Craiului Massif, sample 145. h Complex peloidal stromatolite. The

peloids generate a laminar fabric; the peloidal laminae are interca-

lated by dense microbial micrite. Vladusca Valley, Piatra Craiului

Massif, sample 134. Scale bar is 1 mm

c

30 Facies (2013) 59:19–48

123

Facies (2013) 59:19–48 31

123

32 Facies (2013) 59:19–48

123

bodies with variable diameters consisting of concentric

‘‘densely packed micritic envelopes’’. Subsequently, this

enigmatic organism was mentioned in several studies,

being mainly described as having a structure consisting of a

central sparitic core bordered by some micritic layers. Its

systematic position is still debated (e.g., Flugel 1981;

Leinfelder et al. 1993; Schmid 1995; Krajewski 2000).

Flugel (1981) describes this taxon as a symbiosis between a

nubeculariid foraminifer and a cyanophycean. It displays a

typical laminated-peloidal cyanophycean structure of the

cortex surrounding amphora-like tubes that represent the

foraminifer’s chambers. In other cases, the micritic enve-

lopes building up the cortex may develop around nuclei of

a different nature, such as small bivalve fragments or tubes

of uncertain systematic affiliation. In the samples collected

from the two study areas, this taxon is extremely abundant

in the microbial crusts; most of the specimens display the

typical structures described by Senowbari-Daryan et al.

(2008). We have also noticed tube-shaped structures

showing Crescentiella-type features (e.g., Labes atramen-

tosa Eliasova; Fig. 10e, f) similar to some of the taxa

described by Schlagintweit and Gawlick (2009) from Late

Jurassic reefal carbonates of the Northern Calcareous Alps

(Austria). In contrast to most of the micro-encrusters

identified in the two sections, Crescentiella morronensis

may be also present as isolated structures with no con-

nection to microbial crusts.

Crescentiella morronensis is stratigraphically distrib-

uted in the Oxfordian-Barremian (up to Gargasian;

e.g., Schlagintweit et al. 2012) interval, with an acme in

the Kimmeridgian–Tithonian. This micro-encruster was

described for the first time by Crescenti (1969) from

Tithonian limestones of the Central Apennine Mountains,

Italy. Other typical Tethysian domain carbonate deposits

containing this micro-encruster are Upper Jurassic–Lower

Cretaceous limestones in many other regions (Table 2).

Koskinobullina socialis Cherchi and Schroeder, 1979

Fig. 10e–h

Besides its typical occurrence in microbial crusts, K.

socialis may be also common in oncoidal structures

(Leinfelder et al. 1993). Some authors, e.g., Dupraz and

Strasser (1999), regarded the systematic position of this

micro-organism as uncertain. Originally, K. socialis has

been assigned to algae (Cherchi and Schroeder 1979).

Helm et al. (2003) described K. socialis as consisting of

hemispheric chambers with calcitic walls arranged into

encrusting multilamellar layers. Such crusts, representing

colonies of small vesicular specimens, may develop on

various substrates (Radoicic 2005). In our samples, we

have identified K. socialis within the microbial crusts. It is

commonly associated with other encrusters or microbial

structures, as a binder of the coral-microbial facies. As

compared to other micro-encrusting organisms, this taxon

displays small structures; nevertheless, in association with

L. aggregatum, bacinellid-type structures or Crescentiella

it can form dense crusts within the Stramberk-type lime-

stones of both Buila-Vanturarita and Piatra Craiului

massifs.

Fig. 9 Microencrusters and frame builders from the limestones of the

Piatra Craiului Massif. a Coral fragments, longitudinally sectioned.

Bacinellid structures (B) and Lithocodium aggregatum (L) are

disposed between the corals. b Branching corals surrounded by

common crusts made up of Lithocodium aggregatum (L) associated

with Troglotella incrustans (Ti). The sediment in between corals

contains encrusting organisms and algae (Cresecentiella morronensis(arrows) and Solenopora sp. (S). c Peloidal bioclastic bioconstruction

with Crescentiella morronensis and Mercierella dacica (arrows).

d Serpulid worm tubes (arrows) and Crescentiella morronensis (C) in

a rudstone. e Internal sediment colonized by Crescentiella morron-ensis (arrow) supporting the reefal framework. f Sponge fragment

encrusted by Lithocodium aggregatum (L) and Perturbatacrusta leini(P). g Coral microbial boundstone; the sediment binding the corals is

a peloidal bioclastic wackestone with Radiomura cautica (R) and

worm tubes. h Gastropod skeleton with geopetal infilling; encrusting

foraminifera and Lithocodium aggregatum (L) form an associated

crust around this bioclast. a–h, Vladusca Valley, Piatra Craiului

Massif; a sample 35; b sample 68; c sample 10; d sample 50; e sample

12; f sample 107; g sample 33; h sample 85. Scale bar is 1 mm

b

Table 3 Koskinobullina socialis occurrences within the Tethyan domain

Author Zone Age Country

Radoicic (2005) Mirdita region Lower Valanginian Albania

Schlagintweit and Gawlick (2008) Plassen carbonate platform, Northern Calcareous Alps Upper Tithonian–Lower Berriasian Austria

Helm and Schulke (1998),

Helm et al. (2003)

Suntel Mountains Oxfordian–Tithonian Germany

Rusciadelli et al. (2011) Marsica area, Central Apennines Kimmeridgian–Tithonian Italy

Shiraishi and Kano (2004) Shikoku Island Upper Jurassic–Lower Cretaceous Japan

Matyszkiewicz and Słomka (2004) Outer Carpathians Tithonian–Berriasian Poland

Sasaran et al. (2000, 2001) Trascau Mountains Upper Jurassic–Lower Cretaceous Romania

Uta and Bucur (2003) Buila-Vanturarita Massif, Southern Carpathians Kimmeridgian–Tithonian

Bucur and Sasaran (2011) Haghimas Massif, Eastern Carpathians Berriasian-Valanginian

Facies (2013) 59:19–48 33

123

34 Facies (2013) 59:19–48

123

Koskinobullina socialis is a wide-spread micro-encrus-

ter, being described in several Tethys areas. The first record

was by Cherchi and Schroeder (1979), who found it in

Barremian limestones from Sardinia. Other occurrences are

listed in Table 3.

Lithocodium aggregatum Elliott, 1956 Fig. 11a–d

Lithocodium aggregatum was first described by Elliott

(1956), who assigned it to Codiaceae algae. Leinfelder

et al. (1993) interpreted that this form as an encrusting

organism with a central cavity and an external rim with

radial or bifurcated filaments. In the last decades, the sys-

tematic assignment of this taxon has been intensely deba-

ted. Camoin and Maurin (1988) and subsequently Riding

(1991) admitted the possibility of a microbial origin.

Schmid and Leinfelder (1995, 1996) regarded Lithocodium

as encrusting foraminifers belonging to Loftusiacea, while

Koch et al. (2002) considered it to be a sponge. Cherchi

and Schroeder (2006) have assigned this form to some

colonial calcimicrobial structures (colonies of calcified

cyanobacteria). In recent studies (Schlagintweit 2010,

2011; Cherchi and Schroeder 2010), L. aggregatum sensu

Schmid and Leinfelder (1996) is interpreted as sponge

borings (Entobia) within microbial crusts. Moreover,

Schlagintweit et al. (2010) considered L. aggregatum sensu

Elliott to be an ulvophycean green algae with ‘‘septate

prostrate and erect-branching filaments’’. According to the

last authors, the non-microbial origin of this micro-organ-

ism is proven by the lack of laminated, grumelous or

peloidal microbial microfabrics. In our samples,

L. aggregatum is commonly associated with Bacinella-type

structures and other encrusting micro-organisms (e.g.,

Troglotella incrustans), developing crusts within the coral-

microbial bioconstructions.

The stratigraphic range of L. aggregatum Elliott is

attributed to the (Oxfordian?) Tithonian-Coniacian inter-

val; the Triassic and some of the Upper Jurassic specimens,

which were interpreted as L. aggregatum (e.g., Senowbari-

Daryan 1984), are considered to belong to another taxon

due to the lack of typical morphology as seen in Elliott0smaterial (Schlagintweit et al. 2010, 2011). This micro-

organism has been described from Upper Jurassic–Lower

Cretaceous carbonate deposits of the whole Tethyan area,

from Morocco (Scheibner and Reijmer 1999) to Japan

(Shiraishi and Kano 2004). Elliott (1956) described the

taxon from Lower Cretaceous limestones near Basra, Iraq.

The systematic review of Schlagintweit et al. (2010) was

based on specimens identified in Aptian limestones of the

Maestrat Basin, Spain from where Segonzac and Marin

(1972) also described L. aggregatum. This micro-organism

was also discovered in other regions presented in Table 4.

Bacinella—type structures Fig. 11e–h

Bacinella irregularis has been described by Radoicic

(1959) from Barremian–Aptian deposits of the Dinarid area

(Bosnia). Some authors (Grotsch and Flugel 1992; Helm

and Schulke 1998; Uta and Bucur 2003) assigned a

Table 4 Lithocodium aggregatum occurrences within the Tethyan domain

Author Zone Age Country

Radoicic (2005) Mirdita region Lower Valanginian Albania

Mu (1986) Xainza and Bangon areas Lower Cretaceous China

Helm and Schulke (1998) Suntel Mountains Oxfordian Germany

Cherchi and Schroeder (2006) Khalsi area Upper Aptian India

Immenhauser et al. (2005) Qishn Formation Lower Aptian Oman

Kołodziej (1997) Outer Carpathians Tlthonian–Lower Berriasian Poland

Leinfelder et al. (1993) Lusitanian Basin Kimmeridgian Portugal

Sasaran et al. (2000), Sasaran (2006) Trascau Mountains Upper Jurassic–Lower Cretaceous Romania

Bucur and Sasaran (2011) Haghimas Massif, Eastern Carpathians Berriasian–Valanginian

Schmid and Leinfelder (1995) Betic Cordillera Kimmeridgian–Tithonian Spain

Fig. 10 Microfacies characteristics and encrusting organisms in the

limestone succession of Buila-Vanturarita and Piatra Craiului mas-

sifs. a Longitudinal section through a specimen of Crescentiellamorronensis (C) fixed to a coral; notice the lateral extent of this

specimen; Bistrita Gorges, Buila-Vanturarita Massif, sample 184.

b Longitudinal sections through several specimens of Crescentiella(C) encrusting various small biogenic fragments; Bistrita Gorges,

Buila-Vanturarita Massif, sample P52. c Large specimen of Cres-centiella morronensis (C); Vladusca Valley, Piatra Craiului Massif,

sample 26. d Crescentiella morronensis (C) in oblique section. The

central sparitic tubes are surrounded by concentric, micritic, very fine

peloidal layers. The cortex shows different generations. The inner

layers are darker, while the outer layers are composed of lighter

micrite; Vladusca Valley, Piatra Craiului Massif, sample 115.

e Koskinobullina socialis (K) structure associated with worm tubes;

Bistrita Gorges, Buila-Vanturarita Massif, sample P30. f Crustose

microbial microfacies consisting of Koskinobullina socialis (K) and

Iberopora bodeuri (I) within a Nipponophycus (N) boundstone;

Bistrita Gorges, Buila-Vanturarita Massif, sample 164. g, h Koski-nobullina socialis (K); the encrusted substrate is composed of dark

microbial micrite; g Bistrita Gorges, Buila-Vanturarita Massif,

sample P99; h Vladusca Valley, Piatra Craiului Massif, sample

104. Scale bar is 1 mm

b

Facies (2013) 59:19–48 35

123

36 Facies (2013) 59:19–48

123

microbial origin to these structures, which consist of a

network of micritic filaments and inner voids filled with

sparry calcite. Schlagintweit et al. (2010) have restricted

the term to specific structures that correspond to the type

description of Radoicic (1959). These are assigned to

euendolithic algae with the thallus consisting of cylindrical

filaments perforating bioclasts such as corals or L. aggreg-

atum crusts. The specimens we identified in our samples

are more similar to bacinellid-type structures as defined by

Schlagintweit et al. (2010), respectively to some compa-

rable structures that do not fully comply with the original

description and images.

Such structures are abundant in Upper Jurassic–Lower

Cretaceous deposits of the whole Tethys area. Borza (1975)

and Senowbari-Daryan (1984) described Bacinella-type

structures from Upper Triassic deposits of the Western

Carpathians, Slovakia, and Sicily. The Sicilian specimens

were re-interpreted as belonging to a thaumatoporellacean

alga by Schlagintweit and Bover-Arnal (2012). Dupraz and

Strasser (1999) mentioned such structures in a study of

Upper Oxfordian deposits of the Suntel Mountains,

Germany. When studying the Lower Jurassic Jbel Bou

Dahar carbonate platform of Morocco, Scheibner and

Reijmer (1999) mentioned the presence of Bacinella-type

structures often forming associations with Lithocodium-

type crusts. In the Tethys area, other carbonate deposits

containing such structures are listed in Table 5.

Perturbatacusta leini Schlagintweit and Gawlick, 2011

Fig. 12a–d

This encrusting organism has been recently described by

Schlagintweit and Gawlick (2011) from the Upper Jurassic

Plassen carbonate platform of the Northern Calcareous

Alps. P. leini is very similar to R. cautica Senowbari-

Daryan & Schafer, with which it was previously classified.

The major difference is the labyrinthic structure with

interconnected tubes or chambers of variable sizes showing

mainly rounded endings; additionally, this organism does

not have a fibrous wall. The walls of the chambers are

microcrystalline, while the inner space is bordered with

micrite. Its skeleton, showing a non-segmented channel

system, is comparable to the one of an inozoid sponge

(Schlagintweit and Gawlick 2011). In our samples P. leini

occurs in crusts associated with numerous other encrusters

such as C. jachenhausenensis, Lithocodium- and Bacinella-

type structures, or K. socialis.

Regarding its stratigraphic and paleogeographic range,

this microorganism was described from Kimmeridgian-

Tithonian (?Lower Berriasian) limestones of the Northern

Calcareous Alps (Schlagintweit 2011); it was noticed also

in the Upper Jurassic–Lower Cretaceous limestones of the

Trascau Mountains, Romania (Sasaran 2006), and in the

Tithonian–Berriasian carbonate deposits of the Western

Moesian platform, Bulgaria (Ivanova et al. 2008).

Radiomura cautica Senowbari-Daryan and Schafer,

1979 Fig. 12e–h

According to the description of Senowbari-Daryan and

Schafer (1979), this organism consists of several hemi-

spheric or spherical chambers with smooth inner wall

surfaces. Very seldom the chambers are interconnected. As

Table 5 Bacinella-type structures occurrences within the Tethyan domain

Author Zone Age Country

Eliasova (1981) Stramberk Tithonian Czech Republic

Dahanayake (1977) Jura Mountains Lower Kimmeridgian France

Olivier et al. (2004) Pagny sur Meuse region Oxfordian

Elliott (1963) Basra area Albian Iraq

Uta and Bucur (2003) Buila-Vanturarita Massif, Southern Carpathians Kimmeridgian–Tithonian Romania

Sasaran (2006) Trascau Mountains Upper Jurassic–Lower Cretaceous

Bucur and Sasaran (2011) Haghimas Massif, Eastern Carpathians Berriasian–Valanginian

Grotsch and Flugel (1992) Pacific Upper Aptian

Fig. 11 Microfacies characteristics and encrusting organisms in the

limestones of the Buila-Vanturarita and Piatra Craiului massifs.

a Lithocodium aggregatum (L) encrusting a coral, associated with

Troglotella incrustans specimens (Ti); Bistrita Gorges, Buila-Vantu-

rarita Massif, sample P52. b Large Lithocodium aggregatum nodule

(L) with Troglotella incrustans (Ti) inside the cavities; Bistrita

Gorges, Buila-Vanturarita Massif, sample P44. c Thin crust (0.5 mm

in diameter) of Lithocodium aggregatum (L) associated with Cres-centiella morronensis (C); Vladusca Valley section, Piatra Craiului

Massif, sample 70. d Lithocodium aggregatum (L) and Troglotellaincrustans (Ti) encrusting a dissolved coral fragment; Vladusca

Valley, Piatra Craiului Massif, sample 73. e Oncoid made up of

bacinellid structure (B); Bistrita Gorges, Buila-Vanturarita Massif,

sample P22. f Microbial fabric within a boundstone, associated with

Lithocodium (L) and Bacinella-type crusts (B); Bistrita Gorges,

Buila-Vanturarita Massif, sample P54. g Nodule made up of

Bacinella-type structure (B) surrounded by peloidal sediment;

Vladusca Valley, Piatra Craiului Massif, sample 71. h Partially

dissolved coral branch encrusted by Lithocodium aggregatum and

bacinellid structures; Vladusca Valley, Piatra Craiului Massif, sample

35. Scale bar is 1 mm

b

Facies (2013) 59:19–48 37

123

38 Facies (2013) 59:19–48

123

a rule, within a single specimen, the chambers are of equal

size and their infilling is mainly micro-sparitic. The

external wall of the chambers consists of fibrous calcite,

the fibres being perpendicular to the chamber walls.

Scheibner and Reijmer (1999), Serban et al. (2004), Cat-

incut et al. (2010), and Schlagintweit and Gawlick (2011),

described the taxon in a similar way. The systematic

position of R. cautica is still uncertain in spite of several

proposals to assign it to sponges. The specimens we

assigned to R. cautica in samples from Bistrita Gorges and

Vladusca Valley are small, in general only a few mm in

size. They show ovoidal or rounded chambers of homo-

geneous size, which are only rarely interconnected

(Fig. 12f). As a rule, the chambers are filled with sparitic

cement. Radiomura cautica is moderately abundant among

the micro-encrusters identified in the reef bindstones under

study.

Senowbari-Daryan and Schafer (1979) have first time

identified the taxon in Upper Rhetian deposits of the

Northern Calcareous Alps, Austria. Subsequently, Senow-

bari-Daryan (1984) described it from Upper Triassic

limestones of Sicily. This microencruster was also noticed

in the Lower Jurassic limestones from the Jbel bou Dahar

platform, Morocco (Scheibner and Reijmer 1999). This

form is also common in Upper Jurassic—Lower Creta-

ceous reef limestones of Romania (Sasaran and Bucur

Fig. 12 Microfacies characteristics and encrusting organisms in the

limestones of the Buila-Vanturarita and Piatra Craiului massifs.

a Perturbatacrusta leini (P) associated with various micro-encrusters

stabilizing the boundstone; Bistrita Gorges, Buila-Vanturarita Massif,

sample 164. b Detailed view of Perturbatacrusta leini (P). Bistrita

Gorges, Buila-Vanturarita Massif, sample P84. c Perturbatacrustaleini (P) encrusting a small bryozoan fragment, Vladusca Valley-

Piatra Craiului Massif, sample 175. d Detailed microphotograph of

P. leini (P). The chambers filled with calcite spar are connected by

narrow 0.2–0.3-mm-thick perforations; Vladusca Valley, Piatra

Craiului Massif, sample 115. e Fragment of P. leini (P) within a

bioclastic rudstone; Bistrita Gorges, Buila-Vanturarita Massif, sample

174. f, g, h ?Radiomura cautica (R); interconnection (yellow arrow in

f) between two chambers; f Bistrita Gorges, Buila-Vanturarita Massif,

sample P30; g, h Vladusca Valley, Piatra Craiului Massif; g sample

105; h sample 133. Scale bar is 1 mm

b

Fig. 13 Microfacies characteristics and encrusting organisms in the

limestones of the Buila-Vanturarita and Piatra Craiului massifs. a–

d Encrusting sponge C. jachenhausenensis (C) with spar-filled

cavities hardening the coral-microbial bioconstructions from the

studied successions; a–c, Bistrita Gorges, Buila-Vanturarita Massif;

a, c sample P52; b sample P24; d Vladusca Valley-Piatra Craiului

Massif, sample 138. Scale bar is 1 mm

Facies (2013) 59:19–48 39

123

40 Facies (2013) 59:19–48

123

2001; Serban et al. 2004; Sasaran 2006) and Austria

(Schlagintweit and Gawlick 2008). In a more recent paper,

Schlagintweit et al. (2012) identified specimens of R. cau-

tica in Bedoulian/Gargasian (Aptian) carbonate deposits of

the Mirdita zone of Albania.

Other micro-encrusters

Besides the forms mentioned above, some other represen-

tative taxa were identified in the microbial crusts of bio-

constructions of the Buila–Vanturarita and Piatra Craiului

sections: benthic foraminifera (Coscinophragma sp.;

Fig. 14a, b), calcareous algae (T. parvovesiculifera Raineri;

Fig. 14c, d), microproblematica (Labes atramentosa

Eliasova; Fig. 14e, f), Iberopora bodeuri Granier and

Berthou; Fig. 14h), sclerosponges (C. jachenhausenensis

Reitner, Fig. 13a–d; Murania reitneri Schlagintweit; Neu-

ropora lusitanica Termier, Fig. 7g; T. lusitanica Termier

and Termier), bryozoans, and serpulids (Fig. 14g).

Microbial structures

According to Riding (2000), microbial carbonate macro-

fabrics usually can be divided into three main types: lam-

inated microbial structures (stromatolites), clotted

structures (thrombolites), and structureless microbialites

(leiolites). Based on Schmid’s (1996) classification of

microbialites related to the ratio between the main com-

ponents, Flugel (2004) proposed three types of microbial

microfabrics: peloidal, laminitic, and dense (Fig. 15). The

peloidal microstructures are related to the thrombolytic

fabrics. According to the arrangement of peloids, the

thrombolytic fabrics can be divided into poorly structured

thrombolites, purely clotted thrombolites and layered

thrombolites, the latter representing the transition towards

the laminitic microstructures. Leinfelder et al. (1993)

regarded thrombolites to consist exclusively of peloidal

structures. Riding (1991) showed that thrombolites display

a matrix consisting of peloidal crusts that may include

fragments of reef organisms.

The presence of laminitic microstructures is related to

the presence of stromatolites. The latter may consist of

Fig. 14 Microfacies characteristics and encrusting organisms in the

Buila-Vanturarita and Piatra Craiului massifs. a, b The benthic

foraminifer Coscinophragma sp. (arrows) encrusting corals; a,

Bistrita Gorges-Buila-Vanturarita Massif; sample P13b. b, Vladusca

Valley-Piatra Craiului Massif, sample 5. c, d Thaumatoporellaparvovesiculifera (arrows) bridges over sparitic micro-fenestrae

associated with Bacinella-type meshwork; Bistrita Gorges, Buila-

Vanturarita Massif, sample P93. e Detailed view of Labes atramen-tosa; Bistrita Gorges, Buila-Vanturarita Massif, sample P27. f Bio-

clastic-intraclastic rudstone with Labes atramentosa (arrows);

Vladusca Valley, Piatra Craiului Massif; sample 127. g Serpulid

worm tubes (arrow) growing on a partially dissolved coral fragment;

the serpulids are further encrusted by Crescentiella and Lithocodium.

Bistrita Gorges, Buila-Vanturarita Massif; sample P5. h Biogenic

encrustation made-up of Iberopora bodeuri (arrow), worm tubes, and

cyanobacterial-like structures; it shows some affinity to Pseudoroth-pletzella schmidi Schlagintweit & Gawlick. Bistrita Gorges, Buila-

Vanturarita Massif, Sample P89. Scale bar is 1 mm

b

Fig. 15 Simplified

classification of Mesozoic

microbial structures (modified

from Flugel 2004)

Facies (2013) 59:19–48 41

123

either peloids (peloidal stromatolites), or micritic laminae

most probably resulting from microbial activity (Fig. 8).

The stromatolitic fabrics may be associated with throm-

bolytic fabrics; the resulting structures show a variable

degree of lamination (Riding 1991). Nevertheless, the

presence of microbial structures in our samples from both

sections is subordinated to that of the encrusting micro-

organisms. In the Cheile Bistritei section (Buila–Vantu-

rarita Massif) thrombolytic mesostructures consisting of

peloidal microstructure are dominate. Peloidal stromato-

lites consisting of laminitic microstructures also occur but

not commonly (Fig. 8a, b). In the Vladusca section (Piatra

Craiului Massif) we have identified clotted mesostructures

represented by mesoclots with morphologies varying from

simple spheroids to multi-lobate masses (Fig. 8e–g). The

mesoglomerules consist of diverse microstructures,

including peloids and clotted microfabrics. Additionally,

we noticed laminitic (stromatolitic) mesostructures

consisting of clotted and laminitic micritic microstructures

(Fig. 8h). Occasionally, the stromatolites bind together

other encrusting organisms. In terms of macrofabrics, these

microbial structures are hard to distinguish in field, so our

observations and descriptions are limited to a meso- and

microstructure analysis.

Bioerosion

In the case of the microbial crusts, or even more often in

the case of bioconstructions, bio-erosional features (per-

forations, excavations or micritization) are present. Some

of the resulted empty spaces have been subsequently filled

with geopetal sediment (Fig. 7f). Occasionally, corals

show partly micritized septa as a result of the interaction

with boring-organisms such as bivalves (producing Gas-

trochaenolites), sponges, and foraminifera.

Fig. 16 Pie diagram showing

the percentage distribution of

encrusting organisms in the

sampled section of Buila-

Vanturarita Massif

Fig. 17 Pie diagram showing

the percentage distribution of

encrusting organisms in the

sampled section of Piatra

Craiului Massif

42 Facies (2013) 59:19–48

123

Discussions

The carbonate deposits of Buila-Vanturarita and Piatra

Craiului massifs are built up of thick levels of reef rudstone

interlayered with coral-microbial boundstone. Many of

these reef limestones can be classified as ‘‘coral-microbial-

microencruster boundstones’’ due to their diverse micro-

encruster assemblages and microbial-related structures.

This specific lithofacies type is characteristic of some of

the Intra-Tethyan rimmed platform deposits, long referred

to as Stramberk-type carbonate deposits, or more recent

Plassen-type limestones (Schlagintweit and Gawlick 2008).

In Cheile Bistritei (Buila–Vanturarita), the carbonate

succession is dominated by reef breccias and microbrec-

cias. The bioconstructions form interlayers in the middle

and upper parts of the succession, being installed and

developed on the top of the carbonate breccia facies. As we

have mentioned in the description of the microfacies, the

bioconstructions did not succeed in building a large-scale

vertical framework that would have documented the pres-

ence of a reef paleoslope. The shelf paleoslope can be

connected to the geometry of the inherited basement on

which the carbonate platform formed. In the studied sec-

tions, the microbial crusts and the syndepositional cements,

as part of the micro-frameworks, were responsible for the

stabilization and bounding of the slope-facies types.

Subsequently, the substrate became stable and favorable to

the installation of the coral-microbial bioconstructions. The

coarse reef facies-types (breccia/microbreccia) are evi-

dence of the instability of the shelf-crest slope.

In the carbonate succession of Vladusca (Piatra Craiul-

ui), the vertical succession of the facies associations doc-

uments the gradual transition from reef slope environments

to reef crest ones. At the base and the top of this succes-

sion, the association of bioconstructions with gravity-flow

deposits is evidence of a shelf-slope environment along the

external flanks of the carbonate platform. Towards the top,

bioconstructions become preeminent; the bioclastic-intra-

clastic internal sediment indicates high water energy, thus a

presumed location above the normal wave-base. The

Bacinella-type structures associated to the bioconstructions

at the top of the succession are arguments for gradual

shallowing of the depositional environment (Schmid 1996).

Our data document a gradual transition within the car-

bonate platform from shelf-slope facies to shelf-margin

facies.

Regarding the paleogeographic significance of the ana-

lyzed reef limestones from Buila-Vanturarita and Piatra

Craiului massifs, there are several important aspects that

need to be pointed out. Many studies focusing on Upper

Jurassic microbialite-dominated reefs are referring to the

northern European ramp structures characterized by

Fig. 18 Abundance chart of the

main encrusting taxa from

Buila-Vanturarita Massif. 1Crescentiella morronensis. 2Lithocodium aggregatum. 3Bacinella-type structures. 4Radiomura cautica. 5Perturbatacrusta leini. 6Koskinobullina socialis. 7Coscinophragma sp. 8Calcistella jachenhausenensis

Facies (2013) 59:19–48 43

123

specific facies types and taxa/microencruster assemblages

(Leinfelder et al. 1993, 2002; Reolid et al. 2005; Reolid

and Gaillard 2007). In contrast to this types of carbonate

deposits, the studied successions of the Buila-Vanturarita

and Piatra Craiului massifs are more similar to the rimmed

platforms of the Intra Tethyan realm, with typical micro-

bial crusts and taxonomical associations. The identified

early syndepositional cement microframework (,,cement

crusts’’) and some of the microfossils are characteristic for

the Tethyan domain (Schlagintweit and Gawlick 2008;

Ivanova et al. 2008). Micro-encrusters such as R. cautica or

P. leini are known only in Intra-Tethyan carbonate plat-

forms. Therefore the ‘‘coral-microbial-microencruster

boundstones’’ described in the present paper have more in

common with reefs in Austria (Schlagintweit et al. 2005,

2008), Bulgaria (Ivanova et al. 2008; Roniewicz 2008),

Italy (Rusciadelli et al. 2011), Poland (Kołodziej 1997) and

other regions of Romania (Sasaran 2006) than with reefs on

the northern Tethyan margin. Many coral-microbial reefs

from northern Tethyan domain (France, Switzerland,

Spain) or proto-Atlantic margin (Portugal), are character-

ized by facies with particularly dense microbialites and

laminated macrostructures (Leinfelder et al. 1993), which

are less common within our studied successions from the

Buila-Vanturarita and Piatra Craiului massifs The presence

of the reef breccias and microbreccias levels in the studied

successions can be linked with the progradation of the

carbonate platform during the Late Jurassic, documented

by gradual transition from reef slope to reef crest envi-

ronments. The same features were noticed in the Northern

Calcareous Alps (Schlagintweit and Gawlick 2008), in

contrast to reefs from Portugal which lack of these reef

breccias. The studied carbonate successions, together with

some other deposits from Romania (Uta and Bucur 2003;

Sasaran 2006), are equivalent to those described by

Schlagintweit and Gawlick (2008) as ‘‘microbial-cement-

microencruster boundstones’’ from Austria, also known as

Plassen-type limestones. They are referred to a fore-reef/

upper slope depositional setting and an assumed step slope

gradient. Last but not the least, our samples show close

resemblances to the Ellipsactinia facies of the Central

Apennines with similar microfacies types and microfossil

assemblages (Rusciadelli et al. 2011).

The distribution diagrams and abundance charts of the

main encrusters (Figs. 16, 17, 18, 19) from the Buila–

Vanturarita and Piatra Craiului sections show that C.

morronensis volumetrically dominates the microbial

crusts. Most commonly, Crescentiella encrusted bioclasts

such as corals, bryozoans, or foraminifers. It played a

significant role in the stabilization of sediment within

open environments (Shiraishi and Kano 2004). Lithoco-

dium aggregatum occurs isolated or associated with bac-

inellid structures, forming crusts mainly related to coral

fragments.

Fig. 19 Abundance chart of the

main encrusting taxa from

Piatra Craiului Massif. 1Crescentiella morronensis. 2Radiomura cautica. 3Lithocodium aggregatum. 4Bacinella-type structures. 5Perturbatacrusta leini. 6Koskinobullina socialis. 7Coscinophragma sp. 8Calcistella jachenhausenensis

44 Facies (2013) 59:19–48

123

Even though most of the micro-encrusters contributing

to the microbial crusts in the Upper Jurassic limestones are

well known, some of them are still poorly understood,

especially concerning their systematic position. This aspect

was intensely debated in the last decades (e.g., Schmid

1996; Hoffmann et al. 1997, 2008; Leinfelder et al. 2002;

Schlagintweit et al. 2005, 2010; Schlagintweit and Gawlick

2007, 2009; Cherchi and Schroeder 2006; 2010).

Conclusions

1. The Upper Jurassic carbonate deposits from the Buila–

Vanturarita and Piatra Craiului sections mainly consist

of massive reef limestones. Besides corals, a wide

range of encrusting micro-organisms (C. morronensis,

L. aggregatum, bacinellid structures, R. cautica, P.

leini, K. socialis) and microbial structures, have con-

tributed to their development. The major results of

microbial activity in the reef limestones from the

studied areas were the generation of structures such as

stromatolites, thrombolytic crusts, void infillings, and

peloidal or micritic fabrics, accompanied by various

types of crusts.

2. The identified associations of calcareous algae and

benthic foraminifera allowed us to assign ages to the

studied sections. The limestones from the Buila-

Vanturarita Massif are Kimmeridgian–Tithonian in

age, while those from Piatra Craiului are Kimmerid-

gian-Berriasian–?Lower Valanginian in age.

3. The microfacies analyses corroborated with the com-

position of the taxonomic associations identified in the

studied samples point to similar depositional environ-

ments in the two areas during the Upper Jurassic.

4. Based on their general features, the studied limestones

can be overall assigned to the ‘‘coral-microbial-

microencruster boundstones’’, displaying many resem-

blances with other carbonate deposits of the

Intra-Tethyan domain (Schlagintweit et al. 2005;

Sasaran 2006; Schlagintweit and Gawlick 2008). This

fact, among many, contributes to our knowledge of the

Late Jurassic reefs of the southern-Intra Tethyan

domain, which are still insufficiently documented in

comparison with Late Jurassic reefs from the northern

Tethyan margin.

5. The relative abundance of encrusting micro-organisms

and of microbial structures can be correlated with low

sedimentary rates. The higher the ratio of microbial

crusts among the biotic components of the reef, the

lower the assumed sedimentary rate should be. The

micro-encrusters have played a key role in shaping the

reef morphologies during the Late Jurassic. Their

general traits suggest that most probably, they were

controlled by fluctuations in bathymetry, water energy,

salinity, and nutrient contents. Besides the micro-

encruster consortium, the microbial structures have

stabilized the carbonate platform slopes and provided

support for the development of the bioconstructions.

They also contributed to the reinforcement of the reef

framework, in association with other encrusting micro-

organisms.

6. In spite of the many similarities between the two

analyzed successions concerning microfossil associa-

tions, microfacies characteristics and depositional

environments, we have also documented some distinc-

tive traits such as the taxonomic diversity of the

encrusting organisms: the samples collected from

Buila-Vanturarita show a bigger diversity compared

to those collected from Piatra Craiului.

Acknowledgments This work was possible with the financial sup-

port of the Sectoral Operational Programme for Human Resources

Development 2007–2013, co-financed by the European Social Fund,

under the project number POSDRU/107/1.5/S/76841 with the title

,,Modern Doctoral Studies: Internationalization and Interdisciplina-

rity’’, and through PN-II-ID-PCE-2011-3-0025 grant. We like to thank

Vlad Ples for assistance in the field and Lucian Pascariu and Filip Dima

for their support in sample preparation. We are grateful to Felix

Schlagintweit and Bogusław Kołodziej for their suggestions and

helpful reviews. We also kindly thank Dana Pop for English translation

and Stephen Kershaw for English corrections. We thank Felix Schla-

gintweit for information regarding the stratigraphic range of sponges.

References

Bathurst RGC (1971) Carbonate sediments and their diagenesis.

Developm Sediment12. Elsevier, Amsterdam, p 658

Bathurst RGC (1986) Carbonate diagenesis and reservoir develop-

ment: conservation, destruction and creation of pores. In:

Bathurst RGC, Land LS (eds) Carbonate depositional environ-

ments. Modern and ancient. Part 5: diagenesis 1. Colorado

School Mines, Quart, pp 1–24

Beccaro P, Lazar I (2007) Oxfordian and Callovian radiolarians from

the Bucegi Massif and Piatra Craiului Mountains (Southern

Carpathians, Romania). Geol Carpat 58:305–320

Boldor C, Stilla A, Iavorschi M, Dumitru I (1970) New data regarding

the stratigraphy and tectonics of the Mesozoic sedimentary

deposits from Olanesti (Southern Carpathians). D S Sed Inst

Geol 55(for 1966–1967):217–221 (in Romanian)

Borza K (1975) Mikroproblematika aus der oberen Trias der

Westkarpaten. Geol Carpat 26:199–210

Bucur II (1978) Microfacies of white limestones from the northern

part of Piatra Craiului Massif. Biostratigraphical remarks. D S

Sed Inst Geol 64(for 1976–1977):89–105 (in Romanian)

Bucur II (1980) Rhaxella sorbyana (Blake) in Oxfordian radiolarites

from Piatra Craiului Massif. D S Sed Inst Geol Geophys 65(for

1977–1978):31–35 (in Romanian)

Bucur II (1999) Stratigraphic significance of some skeletal algae

(Dasycladales, Caulerpales) of the Phanerozoic. In: Farinacci A,

Lord AR (eds) Palaeopelagos Spec Publ, vol 2. pp 53–104

Bucur II, Sasaran E (2005) Micropaleontological assemblages from

the Upper Jurassic–Lower Cretaceous deposits of Trascau

Facies (2013) 59:19–48 45

123

Mountains and their biostratigraphic significance. Acta Paleont

Rom 5:27–38

Bucur II, Sasaran E (2011) Upper Jurassic–Lower Cretaceous algae of

Haghimas Mountains (Lacu Rosu-Cheile Bicazului area). In:

Bucur II, Sasaran E (eds) Calcareous algae from Romanian

Carpathians, 10th International Symposium on Fossil Algae,

Cluj Napoca, Romania 12–18 September 2011, Field Trip Guide

Book, Presa Universitara Clujeana, Cluj-Napoca, pp 57–97

Bucur II, Hoffman M, Kołodziej B (2005) Upper Jurassic–lowermost

Cretaceous benthic algae from Tethys and the European

Platform: a case study from Poland. Rev Esp Micropaleontol

37:105–129

Bucur II, Sasaran E, Iacob R, Ichim C, Turi V (2009) Upper Jurassic

shallow water carbonate deposits from some Carpathian areas:

new micropaleontological results. The 8th Symposium of IGCP

506, Abstracts and Field Guide, Editura Universitatii Bucuresti,

Bucuresti, pp 13–14

Bucur II, Sasaran E, Balica C, Beles D, Bruchental C, Chendes C,

Chendes O, Hosu A, Lazar DF, Lapadat A, Marian AV,

Mircescu C, Turi V, Ungureanu R (2010) Mesozoic carbonate

deposits from some areas of the Romanian Carpathians—case

studies. Presa Universitara Clujeana, Cluj Napoca, p 203

Camoin G, Maurin AF (1988) Role des micro-organismes (bacteries,

cyanobacteries) dans la genese des ‘‘Mud Mounds’’. Exemple du

Turonien des Jebels Bireno et Mrhila (Tunisie). CR Acad Sci

307:401–407

Carras N, Georgala D (1998) Upper Jurassic to Lower Cretaceous

carbonate facies of African affinities in a peri-European area:

Chalkidiki Peninsula, Greece. Facies 38:153–164

Catincut C, Michetiuc M, Bucur II (2010) Microfacies and micro-

fossils of the Upper Tithonian–Lower Berriasian calcareous

klippes from Ampoitei Valley (West of Alba Iulia, Romania).

Acta Paleont Rom 7:77–86

Cherchi A, Schroeder R (1979) Koskinobullina n.gen., microorgan-

isme en colonie incertae sedis (Algues?) du Jurassique-Cretace

de la region mediterraneenne; note preliminaire. Bull Centre

Rech Elf Explor Prod 3:519–523

Cherchi A, Schroeder R (2006) Remarks on the systematic position of

Lithocodium Elliott, a problematic microorganism from the

Mesozoic carbonate platform of the Tethyan realm. Facies

52:435–440

Cherchi A, Schroeder R (2010) Boring sponges (Entobia) in Mesozoic

Lithocodium calcimicrobial crusts. Riv Ital Paleont Strat

116:351–356

Coniglio M, Dix GR (1992) Carbonate slope. In: Walker RG, James

NP (eds) Facies models, response to sea level change. Geol

Assoc Canada, pp 349–373

Crescenti U (1969) Biostratigrafia delle facies Mesozoiche dell’Ap-

pennino Centrale: Correlazioni. Geol Romana 8:15–40

Dahanayake K (1977) Classification of the oncoids from the Upper

Jurassic carbonates of the French Jura. Sediment Geol

18:337–353

Dimitrescu R, Patrulius D, Popescu I (1971) Geological map of

Romania, 1:50 000, sheet 110c, Inst Geol Geophys, Bucuresti (in

Romanian)

Dimitrescu R, Popescu I, Schuster CA (1974) Geological map of

Romania, 1:50 000, sheet 110a, Inst Geol Geophys, Bucuresti (in

Romanian)

Dragastan O (1969) Micro-oncolithes dans le Jurassique superieur de

la vallee du Bicaz, Carpates Orientales, Roumanie. Bull Soc

Geol France 11(7):635–639

Dragastan O (1975) Upper Jurassic and Lower Cretaceous microfa-

cies from the Bicaz Valley basin (East Carpathians). Mem Inst

Geol Geophys 21:1–87

Dragastan O (1980) Calcareous algae from the Mesozoic and tertiary

of Romania. Ed Acad RS Romania p 167 (in Romanian)

Dragastan O (2010) Getic carbonate platform—stratigraphy of

Jurassic and lower Cretaceous, reconstructions, paleogeography,

provinces and biodiversity. Editura Universitatii din Bucuresti,

p 622 (in Romanian)

Dupraz C, Strasser A (1999) Microbialites and micro-encrusters in

shallow coral bioherms (Middle to Late Oxfordian, Swiss Jura

Mountains). Facies 40:101–130

Einsele G (1991) Submarine mass flow deposits and turbidites. In:

Seilacher A, Einsele G, Ricken W (eds) Cycles and events in

stratigraphy. Springer, Berlin, pp 313–339

Eliasova H (1981) Some binding microorganisms of the Stramberk

reef limestones (Tithonian, Czechoslovakia). Vest Ustred ust

geol 56:113–128

Elliott GF (1956) Further records of fossil calcareous algae from the

Middle East. Micropaleontology 2:327–334

Elliott GF (1963) Problematical microfossils from the Cretaceous and

Paleocene of the Middle East. Palaeontology 6:293–300

Enos P, Moore CH (1983) Fore—reef slope environment. In: Scholle

PA, Bebout DG, Moore CH (eds) Carbonate depositional

environments. AAPG, Mem 33:508–537

Flugel E (1981) Tubiphyten’’ aus dem frankischen Malm. Geol Bl

NO-Bayern 31:126–142

Flugel E (2004) Microfacies of carbonate rocks. Analysis interpre-

tation and application. Springer, Berlin, p 976

Flugel E, Koch R (1995) Controls on the diagenesis of Upper Triassic

carbonate ramp sediments: Steinplatte, Northern Alps (Austria).

Geol Palaont Mitt Innsbruck 20:283–311

Gawlick HJ, Missoni S, Schlagintweit F, Suzuki H, Frisch W, Krystyn

L, Blau J, Lein R (2009) Jurassic tectonostratigraphy of the

Austroalpine Domain. J Alp Geol 50:1–152

Ginsburg RN, Harris PM, Enerli GP, Swart PK (1991) The growth

potential of a bypass margin, Great Bahama Bank. J Sediment

Petrol 61:976–987

Grammer GM, Ginsburg RN, McNeill DF (1991) Morphology and

development of modern carbonate foreslopes, Tongue of the

Ocean, Bahamas. In: Larue DK, Draper G (eds) Transactions of

the 12th Caribbean Geological Conference, pp 27–32

Grotsch J, Flugel E (1992) Facies of sunken Early Cretaceous atoll

reefs and their capping Late Albian drowning succession

(Northwestern Pacific). Facies 27:153–174

Hammer Ø, Harper DAT, Ryan PD (2001) PAST: paleontological

statistics software package for education and data analysis.

Palaeont Electron 4:9–18

Helm C, Schulke I (1998) A coral-microbialite patch reef from the

Late Jurassic (florigemma-Bank, Oxfordian) of NW Germany

(Suntel Mountains). Facies 39:75–104

Helm C, Schulke I, Schlagintweit F (2003) Calcareous algae

(Porostromata, Rhodophyta, Dasycladales) and microprob-

lematica with algal affinity from the NW German Koralle-

noolith Formation (Oxfordian, Suntel Mountains). Facies

49:61–86

Hoffmann M, Kołodziej B, Matyszkiewicz J (1997) Upper Jurassic

microbolites—examples from the Holy Cross Mts. and Cracow

upland. In: Bednarczyk J, Gradzinski N, Hoffmann M, Jasio-

nowski M, Kołodziej B, Matyszkiewicz J, Paszkowski M, Szulc

J, Wysocka A (eds) 3rd Regional Symposium of International

Fossil Algae Associations, Cracow, Poland, 14–20 September

1997, Guidebook & Abstracts, Institute of Geological Sciences,

Jagiellonian University, Cracow, pp 16–22

Hoffmann M, Kołodziej B, Bucur II, Sasaran E (2008) Rola

mikrobialitow, mikroinkrusterow oraz synsedymentacyjnych

cementow w tworzeniu raf z wapieni typu sztramberskiego z

Polski i Rumunii. In: Utwory przełomu jury i kredy w

zachodnich Karpatach fliszowych polsko-czeskiego pogranicza.

Jurassica VII, _Zywiec/Stramberk, 27–29.09.2008, vol 3. Kwar-

talnik AGH Geol, pp 178–179

46 Facies (2013) 59:19–48

123

Hopkins JC (1977) Production of foreslope breccia by differential

submarine cementation and downslope displacement of carbon-

ate sands, miette and ancient wall buildups, Devonian, Canada.

SEPM Spec Publ 25:155–170

Immenhauser A, Hillgartner H, Van Bentum E (2005) Microbial-

foraminiferal episodes in the Early Aptian of the southern

Tethyan realm margin: ecological significance and possible

relation to oceanic anoxic event. Sedimentology 52:77–99

Ivanova D, Kołodziej B, Koleva-Rekalova E, Roniewicz E (2008)

Oxfordian to Valanginian palaeoenvironmental evolution on the

western Moesian carbonate platform: a case study from SW

Bulgaria. Ann Soc Geol Polon 78:65–90

Jekelius E (1938) Das Gebirge von Brasov. An Inst Geol Rom 19:

308–406

Kendall AC (1977) Fascicular-optic calcite: a replacement of bundled

acicular carbonate cements. J Sediment Petrol 47:1056–1062

Kendall AC, Tucker E (1973) Radiaxial fibrous calcite: a replacement

after acicular carbonate. Sedimentology 20:365–389

Keupp H, Jennisch A, Herrmann R, Neuweiler F, Reitner J (1993)

Microbial carbonate crusts—a key to the environmental analysis

of fossil spongiolites? Facies 29:41–54

Koch R, Moussavian E, Ogorelec B, Skaberne D, Bucur II (2002)

Development of a Lithocodium (syn. Bacinella irregularis)—

reef-mound—a patch reef within Middle Aptian lagoonal

limestone sequence near Nova Gorica (Sabotin Mountain,

W-Slovenia). Geologija 45:71–90

Kołodziej B (1997) Boring Foraminifera from exotics of Stramberk-

type limestones (Tithonian–lower Berriasian, Polish Carpathi-

ans). Ann Soc Geol Polon 67:249–256

Krajewski M (2000) Lithology and morphology of Upper Jurassic

carbonate buildups in the Bedkowska Valley, Krakow region,

southern Poland. Ann Soc Geol Polon 70:151–163

Leinfelder R, Nose M, Schmid UD, Werner W (1993) Microbial

crusts of the Late Jurassic: composition, palaeoecological

significance and importance in reef construction. Facies 29:

195–230

Leinfelder R, Schmid UD, Nose M, Werner W (2002) Jurassic reef

patterns—the expression of a changing globe. In: Kiessling W,

Flugel E, Golonka J (eds) Phanerozoic reef patterns, SEPM Spec

Publ 72:465–520

Lupu M, Popescu B, Szasz L, Hann H, Gheuca I, Dumitrica P,

Popescu GH (1978) Geological map of Romania, 1:50 000, sheet

126a, Vanturarita (Olanesti). Inst Geol Geofiz, Bucuresti (in

Romanian)

Matyszkiewicz J, Felisiak M (1992) Microfacies and diagenesis of an

Upper Oxfordian carbonate buildup in Mydlniki (Cracow area,

Southern Poland). Facies 27:179–190

Matyszkiewicz J, Słomka T (2004) Reef-microencrusters association

Lithocodium aggregatum-Bacinella irregularis from the Cieszyn

limestone (Tithonian-Berriasian) of the Outer Western Carpa-

thians (Poland). Geol Carpath 55:449–456

McIlreath IA, James NP (1984) Carbonate slopes. In: Walker RG (ed)

Facies models. Reprint Series 1:245–257

Meszaros N, Bucur I (1980) Oxfordian nannoplankton from Piatra

Craiului Massif (in Romanian). Muz Bruckenthal St Nat

24:73–77

Mu X-N (1986) Lower Cretaceous calcareous algae from Xainza and

Bangon; northern Xi-Zang. Bull Nanjing Inst Geol Palaeont

Acad Sinica 10:99–105 (in Chinese)

Olivier N, Carpentier C, Bertrand MG, Lathuiliere M, Gaillard C,

Ferry S, Hantzpergue P, Geister J (2004) Coral-microbialite reefs

in pure carbonate versus mixed carbonate-siliciclastic deposi-

tional environments: the example of the Pagny-sur-Meuse

section (Upper Jurassic, Northern France). Facies 50:229–255

Oncescu N (1943) Region de Piatra Craiului-Bucegi. Etude geolog-

ique. An Inst Geol Rom 19:3–124

Patrulius D (1957) Correlation of Upper Dogger and Malm from

Eastern Carpathians. Bul St Acad RPR 2:261–273 (in Romanian)

Patrulius D (1969) Geology of Bucegi Massif and Dambovicioara

Couloir. Editura Academiei RS R, Bucuresti (in Romanian)Patrulius D, Dimitrescu R, Popescu I (1971) Geological map of

Romania, 1:50 000, sheet 110d, Inst Geol Geophys, Bucuresti (in

Romanian)

Pomoni-Papaioannou PF, Flugel E, Koch R (1989) Depositional

environments and diagenesis of Upper Jurassic subsurface

sponge—and Tubiphytes reef limestones: Altensteig 1 well,

western Molasse basin, southern Germany. Facies 21:263–284

Popescu I (1966) Contributions to the knowledge of the stratigraphy

and geological structure of the Piatra Craiului Massif. D S Sed

Inst Geol 52:157–176 (in Romanian)

Radoicic R (1959) Some problematic microfossils from the Dinarian

Cretaceous (in Serbian). Vesnik 17:87–92

Radoicic R (2005) New Dasycladales and microbiota from the

lowermost Valanginian of the Mirdita zone. Ann Geol Penins

Balk 66:27–53

Reolid M, Gaillard C (2007) Microtaphonomy of bioclasts and

paleoecology of microencrusters from Upper Jurassic spongio-

lithic limestones (External Prebetic, Southern Spain). Facies

53:97–112

Reolid M, Gaillard C, Oloriz F, Rodriguez-Tovar FJ (2005) Microbial

encrustations from the Middle Oxfordian–earliest Kimmeridgian

lithofacies in the Prebetic zone (Betic Cordillera, Southern

Spain): characterization, distribution and controlling factors.

Facies 50:529–543

Riding R (1991) Calcified cyanobacteria. In: Riding R (ed) Calcar-

eous algae and stromatolites. Springer, Berlin, pp 55–87

Riding R (2000) Microbial carbonates: the geological record of

calcified bacterial-algal mats and biofilms. Sedimentology

47:179–214

Roniewicz E (2008) Kimmeridgian–Valanginian reef corals from the

Moesian Platform from Bulgaria. Ann Soc Geol Polon

78:91–134

Rusciadelli G, Ricci C, Lathuiliere B (2011) The Ellipsactinia

Limestones of the Marsica area (Central Apennines): a reference

zonation model for Upper Jurassic Intra-Tethys reef complexes.

Sediment Geol 233:69–87

Saller AH (1986) Radiaxial calcite in Lower Miocene strata,

subsurface Enewetak Atoll. J Sediment Petrol 56:743–762

Sandulescu M (1984) Geotectonics of Romania. Editura Tehnica,

Bucuresti (in Romanian)

Sandulescu M, Popescu I, Sandulescu J, Mihaila N, Schuster CA

(1972) Geological map of Romania, 1:50 000, sheet 110b, Inst

Geol Geophys, Bucuresti (in Romanian)

Sasaran E (2006) Upper Jurassic–Lower Cretaceous limestones from

Trascau Mountains. Presa Universitara Clujeana, Cluj Napoca

(in Romanian)

Sasaran E., Bucur II (2001) Upper Jurassic–Lower Cretaceous

microbolites and calcareous algae from the Stramberk-like

limestones in Cheile Turzii area. In: Bucur II, Filipescu S,

Sasaran E (eds) Algae and carbonate platforms in western part of

Romania. Field Trip Guide, 4th Regional Meeting of IFAA,

pp 191–207

Sasaran E, Hosu A, Spalnacan R, Bucur II (2000) Microfacies,

microfossils and sedimentary evolution of the Sandulesti Lime-

stone Formation in Cheile Turzii (Apuseni Mountains, Roma-

nia). Acta Paleont Rom 2:453–462

Sasaran E, Bucur II, Prica I (2001) Microfacies and microfossils in

Upper Jurassic limestones from Cheile Turenilor. Studia UBB

Geol 46:35–52

Scheibner C, Reijmer JG (1999) Facies patterns within a Lower

Jurassic upper slope to inner platform transect (Jbel Bou Dahar,

Morocco). Facies 41:55–80

Facies (2013) 59:19–48 47

123

Schlagintweit F (2010) Taxonomic revision of Late Jurassic ,,Litho-codium aggregatum Elliott’’ sensu Schmid & Leinfelder, 1996.

Jb Geol BA 150:393–406

Schlagintweit F (2011) Taxonomic revision of Late Triassic ,,Litho-codium aggregatum Elliott‘‘(Northern Calcareous Alps, Austria).

Jb Geol BA 151:375–396

Schlagintweit F, Bover-Arnal T (2012) Remarks on BacinellaRadoicic, 1959 (type species B. irregularis) and its representa-

tives. Facies (online first) doi:10.1007/s10347-012-0309-1

Schlagintweit F, Gawlick HJ (2007) Pseudorothpletzella schmidi n.

gen., n. sp.: a new microencruster incertae sedis from Late

Jurassic platform margin/fore-reefal microframeworks of the

Plassen carbonate platform (Northern Calcareous Alps, Austria)

and the Albanides. Jb Geol B A 147:595–605

Schlagintweit F, Gawlick HJ (2008) The occurrence and role of

microencruster frameworks in Late Jurassic to Early Cretaceous

platform margin deposits of the Northern Calcareous Alps

(Austria). Facies 54:207–231

Schlagintweit F, Gawlick HJ (2009) Enigmatic tube-shaped micro-

fossils associated with microbial crusts from Late Jurassic reefal

carbonates of the Northern Calcareous Alps (Austria): a possible

mutualistic sponge-epibiont consortium. Lethaia 42:452–461

Schlagintweit F, Gawlick HJ (2011) Perturbatacrusta leini n.gen.,

n.sp. a new microencruster incertae sedis (?sponge) from late

Jurassic to earliest Cretaceous platform margin carbonates of the

Northern Calcareous Alps of Austria. Facies 57:123–135

Schlagintweit F, Gawlick HJ, Lein R (2005) Mikropalaontologie und

Biostratigraphie der Plassen-Karbonatplattform der Typlokalitat

(Ober-Jura bis Unter-Kreide, Salzkammergut, Osterreich). J Alp

Geol (Mitt Ges Geol Bergbaustud Osterr) 47:11–102

Schlagintweit F, Bover-Arnal T, Salas R (2010) New insights into

Lithocodium aggregatum Elliott 1956 and Bacinella irregularisRadoicic 1959 (Late Jurassic–Lower Cretaceous): two ulvophy-

cean green algae (?Order Ulotrichales) with a heteromorphic life

cycle (epilithic/euendolithic). Facies 56:509–547

Schlagintweit F, Gawlick HJ, Lein R, Missoni S, Hoxha L (2012)

Onset of an Aptian carbonate platform overlying a Middle–Late

Jurassic radiolaritic ophiolithic melange in the Mirdita Zone of

Albania. Geol Croat 65:29–40

Schmid DU (1995) Tubiphytes morronensis—a facultatively encrust-

ing foraminifer with endosymbiotic algae. Profil 8:305–317

Schmid DU (1996) Marine Mikrobolithe und Mikroinkrustierer aus

dem Oberjura. Profil 9:101–251

Schmid DU, Leinfelder RR (1995) Lithocodium aggregatum Elliott

n’est pas une algue mais un foraminifere encroutant, commen-

salise par le foraminifere Troglotella incrustans Wernli &

Fookes. C R Acad Sci Ser 1 320:531–538

Schmid DU, Leinfelder RR (1996) The Jurassic Lithocodiumaggregatum-Troglotella incrustans foraminiferal consortium.

Palaeontology 39:21–52

Segonzac G, Marin P (1972) Lithocodium aggregatum Elliott et

Bacinella irregularis Radoicic de l’Aptien de Teruel (Espagne):

stades de conaissance d’un seul et meme organisme incertae

sedis. Bull Soc Geol France 14(7):331–335

Senowbari-Daryan B (1984) Mikroproblematika aus den obertriadis-

chen Riffkalken von Sizilien. Munster Forsch Geol Palaont

61:1–81

Senowbari-Daryan B, Schafer P (1979) Neue Kalkschwamme und ein

Problematikum (Radiomura cautica n. g., n. sp.) aus Oberrhat-

Riffen sudlich von Salzburg (Nordliche Kalkalpen). Mitt Osterr

Geol Gesell 70:17–42

Senowbari-Daryan B, Bucur II, Schlagintweit F, Sasaran E, Mat-

yszkiewicz J (2008) Crescentiella, a new name for ‘‘Tubiphytes’’

morronensis Crescenti 1969: an enigmatic Jurassic–Cretaceous

microfossil. Geol Croat 61:185–214

Serban D, Bucur II, Sasaran E (2004) Micropaleontological assem-

blages and microfacies characteristics of the Upper Jurassic

limestones from Caprioara-Pojoga (Mures Trough). Acta Pala-

eont Rom 4:475–484

Shapiro RS (2000) A comment on the systematic confusion of

thrombolites. Palaios 15:166–169

Shiraishi F, Kano A (2004) Composition and spatial distribution of

microencrusters and microbial crusts in upper Jurassic–lower-

most Cretaceous reef limestone (Torinosu limestone, southwest

Japan). Facies 50:217–227

Stow DAV (1995) Deep clastic seas. In: Reading HG (ed) Sedimen-

tary environments and facies, 2nd edn. Blackwell, Oxford,

pp 399–444

Todirita-Mihailescu V (1973) Contributions to the study of Creta-

ceous deposits from the north-eastern flank of Vanturarita Ridge

(in Romanian). Anal Univ Bucuresti 22:89–98

Uta A, Bucur II (2003) Microbial structures and microencrusters in

the Upper Jurassic–Lower Cretaceous deposits from Buila-

Vanturarita massif (South Carpathians). Studia UBB Geol 48:

3–14

48 Facies (2013) 59:19–48

123