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ACTA PALAEONTOLOGICA ROMANIAE V. 9 (2), P. 67-84
________________________________
1Babeş-Bolyai University, Department of Geology, Str. M. Kogălniceanu nr. 1, 400084 Cluj-Napoca, Romania, [email protected] 67 2 University of Bucharest, Department of Geology, Bd. Nicolae Bălcescu nr. 1, 010041 Bucharest, Romania, [email protected];
[email protected]; [email protected]
EARLY CRETACEOUS MICROPALEONTOLOGICAL ASSEMBLAGES FROM A
CONDENSED SECTION OF THE CODLEA AREA
(SOUTHERN CARPATHIANS, ROMANIA)
Ioan I. Bucur1*, Eugen Grădinaru2, Iuliana Lazăr2 & Mihaela Grădinaru2
Abstract The “Piatra Mare” quarry near Codlea, Brașov County, Romania, exposes limestones belonging to the
eastern part of the Getic Carbonate Platform. Carbonate deposits consisting of Štramberk-type limestone are here
unconformably overlain by the Braşov Formation. The latter unit starts with a condensed section that overlies a
hardground unconformity on top of the Štramberk-type limestone. We present new results of micropaleontological
investigations of the uppermost part of the Štramberk-type limestone and of the condensed section. Assemblages of
benthic foraminifera, calcareous algae, calpionellids, and calcispheres (cysts of calcareous dinoflagellates) are
identified that enable us to assign a Berriasian–Valanginian age for the studied section. The hiatus identified on the
top of the Štramberk-type limestone is most probably of early Valanginian age.
Keywords: microfossils, foraminifera, calpionellids, calcispheres, Early Cretaceous, Getic Carbonate Platform, Romania
INTRODUCTION
In the eastern part of the Southern Carpathians, carbonate
deposits of the Getic Carbonate Platform are known from
three areas: Braşov-Codlea, Dâmbovicioara-Piatra
Craiului, and the western side of the Bucegi Mountains.
In these areas, the carbonate succession includes deposits
assigned to the Upper Jurassic – Lower Cretaceous.
Commonly, these deposits consist of Štramberk-type
white, massive limestones, considered to have a Late
Jurassic (Kimmeridgian–Tithonian) age (e.g., Popescu,
1967; Patrulius, 1969). Patrulius (1976) and Bucur (1978)
have assumed that Lower Cretaceous (Berriasian–lower
Valanginian) deposits might be also present in these
limestones, a supposition that was subsequently
documented by the fossil record (Patrulius et al., 1980;
Bucur et al., 2009; Dragastan, 2010; Săsăran et al., 2011).
Upper Valanginian–Hauterivian marls were described
overlying the Štramberk-type limestone from both the
Dâmbovicioara (Patrulius, 1969; Patrulius & Avram,
1976; Patrulius et al., 1980) and Braşov-Codlea
(Grădinaru, in Neagu, 1975; Grădinaru & Bărbulescu,
1989; Avram & Grădinaru, 1993; Avram & Grădinaru,
2001; Grădinaru & Bucur, 2001) areas. These two
successions are separated by a condensed section
overlaying a hardground discontinuity at the top of the
Štramberk-type limestones. Patrulius (1969) was the first
to mention the presence of a hardground surface at the
base of the upper Valanginian-Hauterivian deposits in the
Dâmbovicioara area. In the Codlea area, Grădinaru &
Bărbulescu (1989) firstly identified several
discontinuities within the Valanginian-Hauterivian
condensed section unconformably overlying the top of
the Štramberk-type limestone. The detailed microfacies,
sedimentological, geochemical and taphonomical study
of the condensed section and of the associated
discontinuities is still in progress (Mihaela Grădinaru et
al., in preparation), in order to define the depositional
environments characterizing these units of the Getic
Carbonate Platform during the Early Cretaceous. In this
study, we present the micropaleontological assemblages
identified in the Codlea area in samples located towards
the top of the Štramberk-type limestones and in the
condensed section. Based on these results, the aim of the
present paper is to constrain the time duration of the
condensed section and to date the sedimentary hiatus
represented by the hardground unconformity at the top of
the Štramberk-type limestones.
GEOLOGICAL SETTING AND STRATIGRAPHIC
DATA
The studied carbonate rocks are exposed in the small
“Piatra Mare” quarry (Grădinaru & Bărbulescu, 1989;
Avram & Grădinaru, 1993) located at about 2 km south-
west from Codlea (Fig. 1).
The studied section is represented by (Fig. 2):
- white, massive Štramberk-type limestones. Toward the
topmost part, this unit is represented by bioclastic
peloidal grainstone-packstone and bioclastic intraclastic
rudstone. The top of this unit is marked by the first
hardground discontinuity (HG-1) mineralized with
ferruginous crusts (Fig. 2). From this layer, Grădinaru &
Bărbulescu (1989) cited a micropaleontological
association (determined by Dragastan) including
Lithocodium aggregatum, Everticyclammina greigi,
Pseudocyclammina lituus, Ammocycloloculina erratica,
Anchispirocyclina maynci, Protopeneroplis
trochangulata, Trocholina alpina, Trocholina elongata,
Megaporella cf. fluegeli, Paraorthonella richteri,
Rivularia pumilii and Rivularia dianae. The succession
yielding this association was assigned to the Berriasian–
lower Valanginian.
- the base of the Braşov Formation consists of a 10-30 cm
thick condensed section, represented by subnodular to
nodular limestones containing numerous ferruginous
macro-oncoids and a fossil assemblage represented
mainly by brachiopods, ammonites, belemnites, together
with rare bivalves and gastropods. The associated
microfacies types are grey-green to brownish bioclastic
wackestone – packstone with ferruginous ooids and
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
68
Fig. 1 Location of the study area in the Romanian territory and
the geological map of the Codlea town area (modified from
Săndulescu et al., 1972, geological map of Romania, scale
1:50.000, sheet 94d Codlea). 1 - Voinești-Păpușa metamorphic
group; 2 - Permian–Lower Triassic; 3 - Lower Triassic; 4 -
Middle Triassic (Anisian); 5 - Lower Jurassic; 6 - Middle
Jurassic; 7 - Callovian–Oxfordian; 8 - Kimmeridgian–
Tithonian; 9 - Beriassian–Valanginian; 10 - Hauterivian–
Barremian; 11 - latest Albian–Cenomanian; 12 - Pleistocene; 13
- Holocene; 14 - Overthrust line; 15 - Fault; 16 - Quarry. White
arrow points to the „Piatra Mare” quarry.
grapestone structures (Fig. 2). The top of the condensed
layer is marked by the second hardground discontinuity
(HG-2), mineralized with 0.2–0.5 cm-thick ferruginous
laminated crusts. These crusts are distributed along both
hardground discontinuities (HG-1 and HG-2), and they
also occur in fissures, fractures and small neptunian
dykes within the condensed layer. According to Avram
& Grădinaru (1993), the overlying layer consists of a
beige to greenish-white, 10-15 cm thick bioclastic
wackestone-mudstone, followed by 2.3-3 m of yellowish-
gray marls (Fig. 2).
Besides the brachiopod fauna studied by Grădinaru &
Bărbulescu (1989), Avram & Grădinaru (1993)
described from the condensed layer a rich ammonite and
duvaliid fauna ranging in age from latest early
Valanginian to late Valanginian (Verrucosum and
Trinodosum Zones). The ammonites from the overlying
layer are indicative for the latest late Valanginian
Callidiscus Zone (following the ammonite biozonation of
Bulot & Thieuloy, 1994). For the Brașov Formation
marls that follow upwards in the ”Piatra Mare” quarry
succession, the foraminiferal fauna described by Neagu
(1975) indicates a Hauterivian age.
Brief considerations on the identified microfacies and
its depositional significance
The limestone level located below the condensed section
consists of typical shallow water deposits of a carbonate
platform, within which we have identified ooidic-
pisoidic, brecciated peloidal grainstones with keystone
vugs and rivulariacean-type cyanobacteria (Fig. 3a),
intraclastic-peloidal-fenestral limestones with rare, small
foraminifera and meniscus-type cement (Fig. 3b; Fig, 5d),
peloidal-bioclastic, intraclastic grainstone/rudstones with
larger agglutinated foraminifera (Pseudocyclammina and
Spiraloconulus) (Fig. 3c, d), bioclastic-intraclastic
rudstones and bioclastic-peloidal packstone-grainstones,
with micritization rims and early marine fibrous-acicular
cement followed by non-ferroan scalenohedral (”dog
tooth”) calcite cement. The third generation of cement
that surrounds the grains is represented by drusy ferroan
calcite in optical continuity with the scalenohedral
cement. In some voids, the ferroan calcite completely
filled up all the available pore spaces. The matrix is
ferruginized (reddish-brown color), with a variable iron
oxy-hydroxide content (Fig. 3e-h; Fig. 4a; Fig. 5a, b).
Syntaxial calcite overgrowths on echinoderm fragments
are common (Fig. 5f). This cement has generally been
interpreted to be of meteoric diagenetic origin (e.g.,
Bathurst, 1975; Longman, 1980). In addition, the
syntaxial cement grew in competition with the
scalenohedral calcite cement. In some cases, both the
matrix and the grains show traces of dissolution /
recrystallization features (Fig. 5a-c, g), while the fenestral
voids may be filled with successive generations of
sediment, probably including vadose silt. We have also
identified peloidal-bioclastic packstones with
recrystallized grains and brown/reddish matrix showing
cracks filled with finer, hemipelagic brown-reddish
material (Fig. 4c). The fibrous cement indicates
precipitation in marine phreatic environment (James &
Choquette, 1990a). Vadose silt, micrite meniscus and
scalenohedral cements indicate precipitation in vadose
conditions, suggesting significant influence of meteoric
waters (Bathurst, 1975; James & Choquette, 1990b). The
presence of iron oxy-hydroxides surrounding the grains
and intraclasts may by related to subaerial exposure
(Haywick et al., 2009). These features suggest that
diagenesis of the topmost part of the Štramberk-type
limestone was dominated by synsedimentary and early
meteoric processes following short periods of subaerial
exposure. Accordingly, some of these features point to
subaerial exposure stages that have preceded drowning.
The condensed leyer contains fine bioclastic wackestone-
packstones (Fig. 4d) with ferruginous ooids and
clayey micrite matrix (Fig. 4e-h). The associated
micropaleontological content indicates a hemipelagic
(spirillinids, nodosariids, small fragments of molluscs and
echinoderms) to pelagic (calpionellids and calcispheres)
environment.
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
69
The micropaleontological assemblage and its
biostratigraphic significance
Besides sponge fragments (Fig. 5h, i), in the limestone
level located underneath the condensed section we have
identified corals, bryozoans, brachiopods, bivalves,
gastropods and echinoderms, as well as a relatively rich
micropaleontological association. The latter consists
mainly of benthic foraminifera accompanied by
fragments of dasycladaleans and organisms assumed to
have a microbial nature, such as Lithocodium aggregatum
Elliott (Fig. 10n) and bacinellid structures.
The foraminiferal association consists of:
Pseudocyclammina lituus (Yokoyama) (abundant in some
peloidal-bioclastic grainstones) (Fig. 6), Spiraloconulus
suprajurasicus Schlagintweit (Fig. 7), Gaudryina ectypa
Arnaud-Vanneau, Nautiloculina bronnimanni Arnaud-
Vanneau & Peybernes (Fig. 9s), Nautiloculina cretacea
Peybernes (Fig. 9t), Haplophragmoides joukowskyi
Charollais, Brönnimann & Zaninetti (Fig. 8u-w),
Meandrospira favrei Charollais, Brönnimann & Zaninetti
(Fig. 8s, t), Montsalevia salevensis Charollais,
Brönnimann & Zaninetti (Fig. 8j-r), Coscinoconus
alpinus (Leupold) (Fig.9f, g, m), Coscinoconus
cherchiae (Arnaud-Vanneau, Boisseau & Darsac)
(Fig.9d), Coscinoconus delphinensis (Arnaud-Vanneau,
Boisseau & Darsac) (Fig. 9e, h), Coscinoconus molestus
(Gorbatchick) (Fig. 9q), Coscinoconus perconigi Neagu
(Fig. 9i), Protopeneroplis ultragranulata (Gorbachik)
(Fig. 8a, b, d, e, g-i), Protopeneroplis cf. banatica Bucur
(Fig. 8c, f), Neotrocholina valdensis Reichel (Fig. 9n. o),
Mohlerina basiliensis (Mohler) (Fig.10a-d), Earlandia
sp., Glomospira sp., Ammobaculites sp., ?Everticyclamm-
ina sp., Gaudryina sp., Charentia sp., Mayncina sp. (Fig.
9r), Arenobulimina sp., Neotrocholina and Ramulina sp.
(Fig. 9l, p, u)
The species listed above can be grouped into three
categories:
a) Late Jurassic species that are also frequently cited from
the base of the Lower Cretaceous: Pseudocyclammina
lituus, Andersenolina alpina, Protopeneroplis
ultragranulata, Mohlerina basiliensis, Coscinoconus
alpinus, Coscinoconus elongatus (Masse, 1976;
Peybernes, 1976; Azema et al., 1979; Jaffrezo, 1980;
Darsac, 1983; Salvini Bonnard et al., 1984; Boisseau,
1987; Granier, 1987; Arnaud-Vanneau et al., 1988;
Bucur, 1988; Chiocchini et al., 1988; Fourcade &
Granier, 1989; Altiner, 1991; Chiocchini et al., 1994;
Neagu, 1994; Bucur et al., 1995; Bulot et al., 1997;
Gorbachik & Mohamad, 1997; Mancinelli & Coccia,
1999; Ivanova, 2000; Clark & Boudagher-Fadel 2001;
Schlagintweit & Gawlick, 2006);
b) Barremian–Aptian species that are also cited from
Berriasian–Valanginian deposits (Gaudryina ectypa), or
species widely distributed in the entire Lower Cretaceous
(Berriasian–Albian): Nautiloculina bronnimanni and
Nautiloculina cretacea (Arnaud-Vanneau & Peybernes,
1978; Arnaud-Vanneau, 1980; Darsac, 1983; Salvini-
Bonnard et al., 1984; Boisseau, 1987; Bucur, 1988;
Altiner, 1991; Bucur et al., 1995; Bucur et al., 1996; Ebli
& Schlagintweit, 1998);
c) almost exclusively Berriasian–Valanginian species:
Haplophragmoides joukowskyi, Montsalevia salevensis,
Meandrospira cf. favrei, Coscinoconus cherchiae,
Coscinoconus delphinensis, Coscinoconus perconigi,
Neotrocholina valdensis, and Protopeneroplis banatica.
Fig. 2 Lithostratigraphic succession at the base of the Braşov Formation in the „Piatra Mare” quarry, SW
of Codlea town, with location of the samples Cd-1 to Cd-7.
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
70
Fig. 3 Microfacies of the uppermost part of the Štramberk-type limestone. a Ooidic-pisoidic-peloidal grainstone with
keyston-vugs and rivulariacean-type cyanobacteria; sample 160. b Peloidal-intraclastic, fenestral limestone with rare
small foraminifera; meniscus cement can be noticed between some grains; sample 152(a). c, d Peloidal-intraclastic-
bioclastic grainstone with Pseudocyclammina; c, sample J(2); d, sample Nv-2. e-g Intraclastic-bioclastic-peloidal
grainstone; the space between grains is partially filled with a brown-reddish micritic to microsparitic matrix; most of
the grains are surrounded by a fringe of acicular cement; f, sample 106(a); g, sample d-2. h Peloidal-intraclastic-
bioclastic grainstone-packstone. Part of the grains are recystallized and the space in between is partially filled with a
brown-reddish matrix; sample Nc-1. Scale bar: 1mm
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
71
Fig. 4 Microfacies of the limestones at the top of the Štramberk–type limestone (below HG-1) (a, b) and of the
carbonate deposits of the condensed bed in the lower part of the Braşov Formation (c-h). a, b Bioclastic-
intraclastic, and peloidal-intraclastic-bioclastic grainstone-rudstone. Dark brown-reddish to black sediment fills
partially the space between the clasts (in a); the clasts are surrounded by a fringe of acicular white cement. Iron oxi-
hydroxides replaced partially or filled the voids in the carbonate sediment (in b). A, sample 304-1; b, sample 305-1.
c Peloidal-bioclastic packstone with a brown-reddish matrix and fissures (cracks) filled with a finer, brown-reddish
sediment; sample103b. d Fine bioclastic wackestone-packstone marking the drowning of the platform; sample 107-
1. e-h wackestone with iron ooids; e, sample 107-1; f, sample 107-1a; g, sample g-3; h, sample h-3. Scale bar: 1
mm.
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
72
Fig. 5 Microfacies and calcareous sponges from the uppermost part of the Štramberk -type limestones. a Peloidal
packstone with strongly recystallized grains and a brown-reddish matrix; sample Nc-2. b Grainstone-packstone with
a blackish sediment/matrix in the intergranular space; sample 312. c Close-up view of a showing the recrystallized
clasts. d Intertidal peloidal limestone with meniscus cement (arrow); sample 305. e Botioidal, pigmented cement in a
peloidal grainstone; sample 106(a). f Bioclastic-peloidal packstone with a brown-reddish matrix and syntaxial
overgrowth cement on echinoderm plates; sample 314(b). g Dark, iron-rich cement surrounding the recrystallized
grains in a peloidal-bioclastic grainstone; sample 322. h, i Calcareous sponges; h, sample 308a; i, sample 308. Scale
bar: 0.5 mm (a, b, h, i); 0.25 mm (e, d, f, g); 0.125 mm (c).
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
73
Fig. 6 Foraminifera from the uppermost part of the Štramberk-type limestone. a-k Pseudocyclammina lituus
(Yokoyama). Axial-subaxial (a, b, f, i), oblique (c, d, h, j) and subequatorial-equatorial (e, g, k) sections; a, sample
102-1a; b, sample Cd-11; c, sample Nv(2); d, sample 323(a); e, sample Nv(1); f, sample 323(c); g, sample Cd-9; h,
sample 102-1a; i, sample d-2; j, k, sample 316. Scale bar: 0.5 mm (a, c, d, g, i, j); 0.25 mm (b, e, f, h, k).
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
74
Below we present some details on the latter group, given
their significance concerning the age of the studied
limestones.
- Haplophragmoides joukowskyi (Charollais, Brönnimann
& Zaninetti, 1966). Described from Valanginian deposits
(Charollais et al., 1966), Haplophragmoides joukowskyi
has been subsequently identified also in the Berriasian–
Valanginian (Darsac, 1983; Boisseau, 1987; Chiocchini
et al., 1994; Bucur et al., 1995; Ivanova, 2000), as well as
in the Hauterivian (most probably lower Hauterivian)
(Bucur, 1988; Altiner, 1991).
- Montsalevia salevensis (Charollais, Brönnimann &
Zaninetti, 1966). Similarly to H. joukowskyi, this species
was originally described from Valanginian deposits
(Charollais et al., 1966, under Pseudotextulariella
salevensis). Subsequently it was also cited from upper
Berriasian (Salvini-Bonnard et al., 1984: Zaninetti et al.,
1987; Chiocchini et al., 1994) or Hauterivian (probably
lower Hauterivian) formations (Masse, 1976; Peybernès,
1976; Bucur, 1988). However, the great majority of
references for this species concern Valanginian deposits
(Azema et al., 1977; Vila, 1980; Darsac, 1983; Velić &
Fig. 7 Foraminifera from the uppermost part of the Štramberk-type limestone. a-f Spiraloconulus suprajurasicus
Schlagintweit. Longitudinal and longitudinal-oblique sections (a-d); transverse sections (e, f); a, sample Nv(2); b,
sample Cd-11-1; c, d, sample Cd-11-2; e,f, sample Cd-8. Scale bar: 0.5 mm (a, c, d); 0.25 mm (b, e, f).
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
75
Fig. 8 Foraminifera from the uppermost part of the Štramberk-type limestone and the condensed bed in the lower
part of the Braşov Formation. a, b, d, e, g-i Protopeneroplis ultragranulata (Gorbachick). Axial-subaxial (a-b, g-i)
and oblique-tangential (d, e) sections; a, sample 103a; b, sample 101a; d, sample 102-1b; e, sample 104c; g, sample
105, sample Cd-3d; i, sample 104(b). c, f Protopeneroplis cf. banatica Bucur. Subaxial sections; c, sample 323(b); f,
sample 316. j-r Montsalevia salevensis (Charollais, Brönnimann & Zaninetti). Longitudinal (j-m), oblique (n, o) and
transverse (p-r) sections; j, sample Cd-8; k, sample J(1); l, sample J(3); m, sample Nv(3); n, sample 308; o, sample
102-1b; p, sample J(3); q, sample 313; r, sample 312. s ?Meandrospira sp., sample 104(b). t Meandrospira cf. favrei
(Charollais, Brönnimann & Zaninetti), sample Cd-4a. u-v Haplophragoides joukowskyi Charollais, Brönnimann &
Zaninetti. Axial-subaxial sections; u, sample J(3), v, sample Cd-3a; w, sample 313(a). Scale bar: 0.25 mm.
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
76
Fig. 9 Foraminifera from the uppermost part of the Štramberk-type limestone. a, b Coscinoconus elongatus
(Leupold, in Leupold & Bigler). Longitudinal, slightly oblique sections; a, sample Cd-8; b, sample Cd-10. c
Coscinoconus sp. Longitudinal-oblique sections, sample Cd-11; d Coscinoconus cherchiae (Arnaud-Vanneau,
Boisseau & Drasac). Longitudinal section, sample 161-1. e, h Coscinoconus delphinensis (Arnaud-Vanneau,
Boissau & Darsac). Longitudinal sections; e, sample Nv(2); h, sample 314(a). f, g, m Coscinoconus alpinus
(Leupold, in Leupold & Bigler). Longitudinal sections; f, sample d-2; g, sample 303-1; m, sample 106(c). i
Coscinoconus perconigi (Neagu). Longitudinal section; sample Nv(2). j Coscinoconus cf. chiocchinii (Mancinelli
& Coccia). Longitudinal section, sample 314(b). k Coscinoconus cf. campanellus (Arnaud-Vanneau, Boisseau &
Darsac). Longitudinal section, sample 314(a). l, p, u Bullopora/Ramulina sp. l, p, sample 316; u, sample 316(a). n,
o Neotrocholina valdensis Reichel. Longitudinal sections; n, sample b-2; o, sample 309-1. q Coscinoconus
molestus (Gorbachick). Longitudinal section, sample 316. r ?Mayncina sp. Subaxial section, sample 314(b). s
Nautiloculina broennimanni Arnaud-Vanneau & Peybernès. Subaxial sections, sample 314; t Nautiloculina
cretacea Peybernès. Subaxial section, sample J(3). Scale bar: 0.5 mm (a-d, f-k, m, s, t); 0.25 mm (e, l, n-r, u).
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
77
Fig. 10 Foraminifera (a-e), calcareous algae (f-l) and microproblematica (m, n) from the uppermost part of the
Štramberk-type limestone. a-d Mohlerina basiliensis (Mohler). Subaxial (a, b), tangential (c), and oblique (d)
sections; a, sample J(1); b, sample 101-1; c, sample 323(a); d, sample 102. e Troglotella incrutans Wernli &
Fookes inside a Lithocodium-type structure; sample 105-1. f Salpingoporella praturloni (Dragastan). Fragment in
longitudinal-oblique section; sample 316(a). g-i Pseudocymopolia jurassica (Dragastan). Verticils in transverse
(g), oblique (h) and longitudinal (i) sections. G, sample 323; h, sample 311; i, sanple e-2. j-l Parachaetetes
asvapatii Pia. Longitudinal (j) and oblique (k, l) sections; sample 106(b). m Iberopora bodeuri Granier &
Berthou; sample 104. n Lithocodium aggregatum Elliott; sample 104. Scale bar: 0.25 mm (a-j, m); 0.50 mm (k, l,
n).
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
78
Sokač, 1983; Boisseau, 1987; Chiocchini et al., 1988;
Velić, 1988; Altiner, 1991; Bucur et al., 1995; Ivanova,
2000; Husinec & Sokač, 2006; Schlagintweit & Gawlick,
2006; Granier & Bucur, 2011; Bonin et al., 2012).
Zaninetti et al. (1987), the authors of this genus, were the
firsts to notice its similarity to the genus Montsalevia
(they called this species “Montsalevia” salevensis). Other
authors, such as Altiner (1991), Chiocchini et al. (1994),
Bucur et al. (1995), Bulot et al. (1997), Ivanova (2000),
Schroeder et al. (2000), Schlagintweit & Gawlick (2005,
2006), Husinec & Sokač (2006) or Bonin et al. (2012)
have later supported the assignment to this genus.
- Meandrospira favrei (Charollais, Brönnimann &
Zaninetti, 1966). This taxon was described by Charollais
et al. (1966) under Citaella? favrei, besides H. joukowskyi
and M. salevensis. The species was identified in
Valanginian (Boisseau, 1987; Bucur et al., 1995; Pop &
Bucur, 2001) as well as in upper Valanginian to lower
Hauterivian deposits (Bucur, 1988; Altiner, 1991;
Ivanova, 2000; Ivanova & Kołodziej, 2010).
- Coscinoconus cherchiae (Arnaud-Vanneau, Boisseau &
Darsac, 1988), Coscinoconus delphinensis (Arnaud-
Vanneau, Boisseau & Darsac, 1988) and Coscinoconus
perconigi (Neagu, 1994) are species that were cited
exclusively from Berriasian–Valanginian deposits
(Boisseau, 1987; Arnaud-Vanneau et al., 1988; Altiner,
1991; Chiocchini et al., 1994; Bucur et al., 1995;
Mancinelli & Coccia, 1999); these species were assigned
to the genus Trocholina. Only Coscinoconus delphinensis
was cited from the uppermost Tithonian (Gorbachik &
Mohamad, 1997; Ebli & Schlagintweit, 1998). When
describing the species Andersenolina perconigi, Neagu
(1994) has transferred all these species to the genus
Andersenolina. Recently, Rigaud et al. (2013) have
emphasized the differences between the various genera
included in the Trocholinidae family and have
demonstrated the need for restoring the generic name
Coscinoconus Leupold, in Leupold & Bigler, 1936 for the
species originally assigned to the genus Trocholina and
subsequently to the genus Andersenolina (the latter being
considered a recent synonym of the genus Coscinoconus).
- Neotrocholina valdensis Reichel, 1955. This species
was described from Valanginian deposits (Reichel, 1955)
as the type species for the genus Neotrocholina. It has
been frequently cited from deposits assigned exclusively
to the Berriasian–Valanginian (Vila, 1980; Darsac, 1983;
Boisseau, 1987; Granier, 1987; Bucur, 1988; Chiocchini
et al., 1988; Altiner, 1991; Luperto Sinni & Masse, 1994;
Bucur et al., 1995; Neagu, 1995; Clark & Boudagher-
Fadel, 2001).
- Protopeneroplis banatica Bucur, 1993. P. banatica was
first mentioned (as Protopeneroplis aff. trochangulata)
from Hauterivian deposits (Bucur, 1988); the age of these
deposits has been subsequently revised and assigned to
the late Valanginian–early Hauterivian (Bucur, 1991).
Bucur (1993) provided a detailed description of the
species. This foraminifer is relatively poorly known, in
spite of the fact that it was also noticed in southeast
France (Blanc et al., 1992). Subsequently, the species was
identified in Serbia from Valanginian deposits (Bucur et
al., 1995) as well as in Slovenia, from the Valanginian
and Aptian ones (Bucur, 1997).
- A special mention is due to the species Protopeneroplis
ultragranulata (Gorbachik, 1971). Originally described
from Lower Cretaceous deposits from Crimea
(Gorbachik, 1971) under the name Hoeglundina(?)
ultragranulata, this species has been considered a
synonym of Protopenerolis trochangulata Septfontaine,
1974 by Septfontaine et al. (1991). Bucur (1993)
transferred the species ultragranulata to the genus
Protopeneroplis. While it was considered for long time a
marker for the Berriasian–Valanginian, the species has
been subsequently identified in middle Tithonian (Heinz
& Isenschmidt, 1988) or even lower Barremian (Bucur,
1993, 1997; Arnaud-Vanneau & Sliter, 1995, under
Protopeneroplis sp.) deposits. Nevertheless, the most
Fig. 11 Calpionellids from the condensed bed in the lower part of the Braşov Formation. a-e Calpionella alpina
Lorenz; a, sample Cd-4a; b, sample Cd-7e; c, sample 107; d, sample 318-1; e, sample Cd-4e. f Calpionella elliptica
Cadish; sample 103-1b. g-j Tintinnopsella carpathica (Murgeanu & Filipescu); g, sample 310; h, sample 321-1; i,
sample 302-1; j, sample Cd-4e-1. k Calpionellopsis oblonga (Cadish); sample 319-1. l ?cf. Calpionellopsis simplex
(Colom); sample Cd-7e-1. Scale bar: 0.125 mm.
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
79
frequent occurrence of this species is in the Berriasian–
lower Valanginian (Azema et al., 1977; Azema et al.,
1979; Salvini-Bonnard et al., 1984; Boisseau, 1987;
Granier, 1987; Zaninetti et al., 1988; Bucur, 1988;
Chiocchini et al., 1988; Velić, 1988; Chiocchini et al.,
1994; Bucur et al., 1995). Bucur (1993, 1997) presented a
quasi-complete list of synonyms together with additional
remarks on this species.
- Spiraloconulus suprajurasicus Schlagintweit, 2011, also
has a particular significance. This foraminifer was
described from Upper Jurassic–?Berriasian deposits from
the Northern Calcareous Alps (Schlagintweit, 2011), then
mentioned and figured (under Otaina magna and
Foraminifera X, respectively) from upper Tithonian–
Berriasian deposits in Hăghimaş area (Eastern
Carpathians, Romania) by Bucur et al. (2011) and
Dragastan (2011). The basal Cretaceous limestones from
Codlea currently represent the third area of occurrence
for this species.
Table 1 synthesizes the stratigraphic distribution of the
benthic foraminifera identified in the layer at the top of
the Štramberk-type limestone, below the condensed
section under study. It is obvious from this synopsis that
the whole association can be assigned to the Berriasian–
Valanginian interval. The two dasycladalean algae also
present in the association from the base of the condensed
Stratigraphically, among the cited calpionellids, C. alpina
does not extend beyond the lower Valanginian, while the
upper limit of C. elliptica is the middle Berriasian. The
latter is a biozone species with a constrained stratigraphic
distribution: it has not been identified in deposits older or
younger than the Berriasian. Calpionellopsis simplex is
present in the upper Berriasian and basal Valanginian,
while Calpionellopsis oblonga occurs later in the upper
Berriasian and continues untill the upper part of the lower
Valanginian (Pop, 1994). Concerning the calcispheres,
Cadosina fusca fusca was described from the Tithonian–
Hauterivian, Colomisphaera conferta from the lower
section, i.e., Salpingoporella praturloni (Dragastan,
1971) and Pseudocymopolia jurassica (Dragastan, 1968)
are typical for the Berriasian–Valanginian interval
(Masse, 1976, 1993; Peybernès, 1976; Granier, 1987;
Jafrezo, 1980; Granier & Deloffre, 1993; Bucur et al.,
1995; Bucur, 1999; Dragastan, 1999). Accordingly, they
too emphasize the Berriasian–Valanginian age of this
level.
From the condensed section at the base of the Brașov
Formation (Fig. 2) we have identified several
foraminifera such as Meandrospira cf. favrei (Charollais,
Broennimann & Zaninetti) (Fig. 8t), Spirillina italica
Dieni & Massari (Fig. 12s-u), Nodosaria sp. (Fig. 12v),
Lenticulina sp., as well as an association with
calpionellids and calcispheres, with: Calpionella alpina
Lorenz (Fig. 11a-e), Calpionella elliptica Cadisch (Fig.
11f), Tintinopsella carpathica (Murgeanu & Filipescu)
(Fig. 11g-j), Tintinnopsella cf. longa (Colom), cf.
Calpionellopsis simplex (Colom) (Fig. 11l),
Calpionellopsis oblonga (Cadisch) (Fig. 11k), Cadosina
fusca fusca Wanner (Fig. 12a, b), Colomisphaera
conferta Řehánek (Fig. 12c-f), Stomiosphaera moluccana
Wanner (Fig. 11g), Colomisphaera vogleri Borza (Fig.
12h, i), Crustocadosina semiradiata olzae (Nowak) (Fig.
12j, k), Cadosinopsis nowaki Borza (Fig. 12l), and
Stomiosphaera echinata Nowak (Fig. 12m-r).
Valanginian, Colomisphaera vogleri from the
Valanginian–Aptian, Stomiosphaera echinata from the
Valanginian–Barremian while Crustocadosina
semiradiata olzae is known from the Valanginian–
Hauterivian (Borza & Michalik, 1986; Reháková, 2000a,
2000b). To summarize, the calpionellid – calcisphere
association points to a middle Berriasian–Valanginian–
?Hauterivian age. Although the bulk of the ammonite
fauna coming from the condensed layer belongs to the
Verrucosum and Trinodosum Zones of the late
Valanginian, to which few representatives for the latest
early Valanginian are also added (Avram & Grădinaru,
Table 1. General stratigraphic range of the foraminiferal species identified in the uppermost
part of the Štramberk-type limestone from Codlea.
Ioan I. Bucur, Eugen Grădinaru, Iuliana Lazăr & Mihaela Grădinaru
80
1993), we conclude that the condensed layer also contains
older deposits, i.e., assigned to the middle Berriasian–
lower Valanginian. Our arguments are supported by the
fact that the calpionellids are identified exclusively within
the macro-oncoids originating from the condensed layer
with ferruginous ooids.
Based on the petrographical description of the condensed
section made by Avram & Grădinaru (1993), in which
“intraformational” fragments of marly limestones are
usually present in oncoids, the condensed layer might
represent a transgressive “lag” that reworked older
deposits during the onset of the drowning of the Getic
Carbonate Platform.
CONCLUDING REMARKS
The Lower Cretaceous deposits studied in the „Piatra
Mare” quarry located south of Codlea have been
investigated for their micropaleontological content. We
have identified an assemblage of foraminifera, calcareous
algae, calpionellids and calcispheres that overall indicates
a Berriasian–Valanginian age for these deposits.
However, the micropaleontological record does not
provide unequivocal arguments for timing of the
unconformity present between the Štramberk-type
limestone and the condensed section from the basal part
of the Braşov Formation. The limestones at the top of the
Štramberk-type limestone include species typical for the
upper Berriasian–lower Valanginian interval (e.g.,
Montsalevia salevensis), while the condensed section
includes middle Berriasian (Calpionella elliptica) and
late Berriasian–early Valanginian (Calpionellopsis
oblonga) calpionellids, as well as calcispheres that are
more representative for the upper Valanginian–
?Hauterivian (Colomisphaera vogleri, Stomiosphaera
echinata, or Crustocadosina semiradiata olzae). Under
these circumstances, the unconformity at the base of the
condensed section (HG-1) shall be placed into the
Valanginian time interval, most probably in the early
Fig. 12 Calcispherulids and foraminifera from the condensed bed in the lower part of the Braşov Formation. a, b
Cadosina fusca fusca Wanner; a, sample 107; b, sample 108(2). c-f Colomisphaera conferta Řehánek; c, sample 302-1;
d, sample Cd-10-1; e, sample Cd-7e-1; f, sample Cd-4c. g Stomiosphaera sp., sample108(2); h-i Colomisphaera vogleri
(Borza); h, sample 318(1); i, sample 107-1. j-l Crustocadosina semiradiata olzae (Nowak); j, k, sample 108(2); l,
sample Cd-4e-2. m-r Stomiosphaera echinata Nowak; m, sample Cd-4a; n, sample 108(2); o, sample 302(1); p, sample
Cd-7e-3; q, r, sample 318(1). s-u Spirillina italica Dieni & Massari sp.; s, sample f-3; t, sample 318-1; u, sample Cd-4e-
1. v Nodosaria sp.; sample g-3. Scale bar: 0.125 mm (a-r, t,u); 0.25 mm (s, v).
Early Cretaceous micropaleontological assemblages from a condensed section of the Codlea area (Southern Carpathians, Romania)
81
Valanginian, as already indicated by the ammonite and
duvaliid faunas.
ACKNOWLEDGEMENTS
The study is a contribution to a CNCS project financed
by grant PN-II-ID-PCE-2011-3-0025. We also thank
Felix Schlagintweit (München) for help in identifying
Spiraloconulus suprajurasicus, and the two reviewers,
Wyn Hughes and Mike Kaminski (Dhahran) for their
remarks and corrections.
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