GEOLOGIJA 40, 153-185 (1997), Ljubljana 1998
Lower Cretaceous Shallow-Marine Sedimentation and Biota on
Dinaric Carbonate Platform between Logatec, Krka and Kolpa
(Southeastern Slovenia)
Spodnjekredna plitvomorska sedimentacija, favna in flora na Dinarski
karbonatni platformi med Logatcem, Krko in Kolpo (južnovzhodna Slovenija)
Stevo Dozet & Ljudmila Šribar
Geološki zavod Ljubljana
Inštitut za geologijo, geotehniko in geofiziko
Dimičeva 14, 1000 Ljubljana, Slovenija
Key-words: biostratigraphy, Lower Cretaceous, microfacies, depositional envi-
ronment, Dinaric carbonate platform. Outer Dinarides, southeastern Slovenia
Ključne besede: biostratigrafija, spodnja kreda, mikrofacies, sedimentacijsko
okolje. Dinarska karbonatna platforma, Zunanji Dinaridi, južnovzhodna Slovenija
Abstract
On the basis of detailed biofacies and microfacies analysis of several cross-secti-
ons in the southeastern Slovenia the biostratigraphic subdivision of the Lower Cre-
taceous stratigraphie sequence has been made. In the study area the Lower Cretace-
ous involves five cenozones and four subzones, namely: Clypeina ? solkani, Salpin-
goporella muehlbergii, Salpingoporella dinarica, Orbitolina (Mesorbitolina) ex gr
texana and "Valdanchella" dercourti (cenozones) as well as Favreina salevensis +
Salpingoporella annulata, Epimastopora ? cekici + Cuneolina tenuis, Orbitolinopsis
capuensis and Palorbitolina lenticularis (subzones). The sediments and fossils in the
inner part of the Dinaric carbonate platform point at more or less continual sedi-
mentation, chiefly in very shallow water environments from intertidal to shallow
subtidal. The continuity of the sedimentation was interrupted by sporadic intensifi-
ed intertidal movements and short-lasting emersions.
Kratka vsebina
Na podlagi nadrobne mikrofacialne in biofacialne analize več profilov je
opravljena biostratigrafska razčlenitev spodnjekrednega zaporedja sedimentov.
Na obravnavanem ozemlju obsega spodnja kreda 5 cenocon in 4 podcone, in sicer:
Clypeina ? solkani, Salpingoporella muehlbergii, Salpingoporella dinarica, Orbi-
tolina (Mesorbitolina) ex gr. texana in "Valdanchella" dercourti (cenocone) ter
Favreina salevensis + Salpingoporella annulata, Epimastopora ? cekici + Cuneoli-
na tenuis, Orbitolinopsis capuensis in Palorbitolina lenticularis (podcone). Sedi-
menti in fosili notranjega dela karbonatne platforme kažejo na bolj ali manj zve-
zno sedimentacijo v plitvem podplimskem, medplimskem in nadplimskem okolju.
Sedimentacijo so občasno prekinjali pojačani epirogenetski premiki in kratkotraj-
ne emerzije.
154_Stevo Dozet & Ljudmila Šribar
Introduction
The study area was geologically mapped and reconnoitred for the Geologic map of
Slovenia 1 : 100 000 in the years between 1965 and 1985 by P 1 e n i č a r et al.
(1970), В u s e r (1974), as well as Savie and Dozet (1985). In the frame of the
research programme "Mesozoic of Slovenia" biostratigraphic investigations of the
Lower Cretaceous were performed in the Logatec area (Šribar, 1979a). Detailed
sedimentological investigation (Strohmenger & Dozet, 1991) have been car-
ried out in the section Kompolje-Ogorelec on the Mala gora mountain and in the sec-
tion Krka-Mali Korinj in Suha Krajina about 35 km SSE from Ljubljana. The second
systematic regional geological investigations of the Slovene territory with a purpose
to make the Geologic map of Slovenia on the scale of 1:50 000, involving detailed fi-
eld mapping and accompanying systematic examinations in the Logatec and Suha
Krajina area, is being carried out by Dozet and Stojanovič.
A detailed study and correlation of several geological sections and numerous
useful data obtained in the field during described geological mappings have been
used as a base for the description and biostratigraphic subdivision of the Lower
Cretaceous stratigraphie sequence in the Slovene Karst Dinarides between Loga-
tec, Krka and Kolpa in the Dinaric carbonate platform area. A complete develo-
pment of the Lower Cretaceous comprising the Berriasian to the Upper Albian was
established.
Hydrozoans, sponges and corals have been determined by Dragica Tumšek. Mario
Pleničar determined the rudist macrofauna. The carbonate rocks are classified according
to F o 1 k's (1959) practical pétrographie classification of limestones and D u n h a m's
(1962) classification of carbonate rocks according to depositional texture.
Important Previous Investigations
U r Š i Č (1933) discovered and described coral, rudist and orbitolinid limestones in
the Kočevje area.
Radoičić (1960) was the first to subdivide biostratigraphically the Lower Cre-
taceous beds in the Outer Dinarides. On the basis of microfossil associations, especi-
ally foraminifera and algae, she ranged the beds with tintinnids into the lowermost
part of the Lower Cretaceous (Infravalanginian, Valanginian). She also registered
Hauterivian with Muneiria baconica and Barremian-Aptian with Salpingoporella di-
narica and Bacinella irregularis.
Farinacci and Radoičić (1964) correlated the Jurassic and Cretaceous
beds of the Apennines and the Dinarides. The comparision showed similar paleoeco-
logical conditions of the Jurassic and Lower Cretaceous sedimentation. Nevertheless,
in the Dinarides the zone of aberrant tintinnins is ascribed to Valanginian, whereas
the zone Clypeina jurassica + Bankia striata (tintinnins) in the Central Apennines is
attributed to the Upper Malm.
On the basis of micropaleontological examination of the samples from Trnovski
gozd T u r n š e k and Buser(1966) placed the boundary between the Portlandian
and the Valanginian there where Clypeina jurassica became extinct. The abberant
tintinnins appear already in the Upper Malm but are more frequent in the Valangini-
an. In their opinion, the aberrant tintinnins together with Nerineae disappeared at
the end of Valanginian.
Lower Cretaceous Shallow-Marine Sedimentation and Biota_ 3
In the explanatory text to the map sheet of the Postojna area P 1 e n i č a r et al.
(1970) presented the data and results of systematic geologic mapping for the Geologi-
cal map of Slovenia 1:100 000.
Buser(1974) described the general geology in the Ribnica map sheet area. He
subdivided the Lower Cretaceous succession into the following mapping units: Va-
langinian, Hauterivian and Barremian, Valanginian and Hauterivian, Aptian, Albian
and Cenomanian.
T u r n Š e k and B u s e r (1974) examined and described the Lower Cretaceous
Cnidaria found in several places between Osojnica, Avšček and Levpa on Banjska
planota, which they dated from the Barremian to the Aptian time.
O r e h e k and Ogorelec(1979, 1981) correlated the microfacial and geoche-
mical characteristics of beds of the southern carbonate platform in Slovenia. Accor-
ding to the literature they are within the general limits of carbonate rocks.
According to algal and foraminiferal contents of the Lower Cretaceous succession
from the Logatec plateau Šribar(1979a) recognized five cenozones and one inter-
zone. After she had studied all the aspects of the occurrences of the aberrant tin-
tinnids she attributed the limestones with clypeinas and aberrant tintinnids to the
Upper Malm.
Šribar et al. (1979) described the Lower Cretaceous sediments in the cross-sec-
tion Vrhnika-Logatec. The Lower Cretaceous sedimentaiy rocks begin with the Ber-
riasian stromatolitic dolomites and limestones and end with the Albian bituminous
limestone.
In the area between Kočevje and Krka P 1 e n i č a r and Šribar (1983) proved
by microfossils and rudists the continuous Lower and Upper Cretaceous sedimentary
succession. In the Lower Cretaceous stratigraphie sequence they distinguished the
Berriasian (Favreina salevensis), Valanginian-Hauterivian (Clypeina ? solkani), Bar-
remian (Dasycladaceae), Lower Aptian (Palorbitolina lenticularis), Upper Aptian
(Salpingoporella dinarica), and Albian (Cuneolina pavonia parva).
Savie and Dozet (1985) described the general geology of the Delnice map.
They subdivided the Lower Cretaceous succession into the following mapping units:
limestones and dolomites, calcareous breccias, limestones and dolomites, Barremian
limestones and dolomites, Aptian limestones and Albian limestones.
On the basis of detailed and extensive investigations and by correlation of the ob-
tained results in the wider area Dozet (1990) subdivided the Lower-Cretaceous
stratigraphie sequence of the Kočevje and Gorski Kotar area in five cenozones and
three subzones.
In the Kočevje and Gorski Kotar area Dozet and Šribar (1991) established
and described the uninterrupted Lower Cretaceous sedimentary succession from Ber-
riasian to the Upper Albian carbonate rocks.
Strohmenger and Dozet (1991) studied sedimentologically a complete
succession of the Jurassic beds including the contacts between the Upper Triassic
and the Lower Lias as well as the Upper Malm and Lower Cretaceous.
T u r n Š e k et al. (1992) paleontologically studied the Lower Cretaceous coral, ru-
dist and foraminiferal fauna of Slovenski vrh in the Kočevje area. The authors sup-
posed the Lower Cretaceous coral-rudist reef development on Slovenski vrh most
probably corresponds to the white coral limestone and white yellow chamid limesto-
ne of the second horizon as mentioned byUršič(1933).
156_Stevo Dozet & Ljudmila Šribar
Lower Cretaceous Stratigraphy
In southern Slovenia the Jurassic beds pass gradually into the Lower Cretaceous
ones. The biostratigraphic boundary between the Upper Malm and the Lower Creta-
ceous is rather problematic in the Dinarides. Some authors draw the boundary either
at the appearance of the aberrant tintinnids (Radoičić, 1960; Farinacci &
Radoičić, 1964), after the extinction of Clypeina jurassica (B u s e r, 1968, 1989;
Turnšek & Buser, 1966), or later after the extinction of the aberrant tintinnins
(V e 1 i Ć, 1977; Velie & Sokač, 1978; Šribar, 1979a, b). However, it must be taken
into consideration that these microfossils are rather fades dependent (Radoičić,
1969). Since the treated beds do not show appreciable fades changes we place the bo-
undary between the Upper Malm and the Lower Cretaceous, after the last appearan-
ce of the aberrant tintinnins.
The Lower Cretaceous sedimentary succession of the study area is predominantly
composed of shallow marine carbonates deposited in the inner part of the vast Dina-
ric carbonate platform. Limestones were formed in shallow-marine environments i.e.
lagoon, subtidal, restricted shoals, back-reef, reef and others. Limestones were occa-
sionally more or less late-diagenetically or early-diagenetically dolomitized. Conse-
quently, all transitional types between limestone and dolomite can be observed in the
studied area.
In the study area the complete development of the Lower Cretaceous beds has be-
en found, representing the Berriasian, Valanginian, Hauterivian, Neocomian, Barre-
mian, Lower Aptian, Upper Aptian, Lower Albian and the Upper Albian.
Berriasian
Generally, in the study area four developments of the Berriasian beds can be di-
stinguished: the predominantly dolomitic develoment, the limestone development,
dolomite-limestone development and finally, the dolomite development with chert.
The Berriasian stratigraphie sequence consists of alternating brownish gray, gray,
medium gray, light gray and very light gray sparitic dolomite, laminated stromatolitic
dolomite as well as micritic, dismicritic and intraclastic limestones. Strong dolomiti-
zation is characteristic for the Berriasian rocks. Early diagenetic dolomite is light gray
to white, stratified (40-150 cm), fine-grained, cryptocrystalline to microcrystalline, la-
minated and stromatolitic, containing ostracods, gastropods, oncoids, shrinkage pores,
fecal pellets and birdseyes. The early diagenetic dolomites are often associated with
birdseyes and stromatolitic structures. Intercrystalline pores are generally filled with
late diagenetic blocky calcite. The dolomite is chemically pure with some illite, mon-
tmorillonite and chlorite admixture. Late diagenetic dolomite is chiefly dark gray to
brownish gray, coarse-grained, saccharoidal, without inner structures, occurring in
lens-like or irregular bodies. Both dolomites are encountered relatively frequently and
in great quantities. The Berriasian beds are up to 100 metres thick.
In the limestones, which according to their stratigraphie position belong to Berria-
sian, a low-diversity and predominance of Favreina pellets, peloids and micritic in-
traclasts is characteristic. Abundant birdseyes, stromatolitic structures and gravita-
tional cements occur in the described carbonate sediments. Consequently, the sedi-
ments were chiefly formed in a shallow subtidal, intertidal to supratidal environ-
ments with strong meteoric influx.
Lower Cretaceous Shallow-Marine Sedimentation and Biota_ 157
Valanginian
The Valanginian sedimentary succession chiefly consists of medium gray, gray, and
light gray, stratified, micritic, pelmicritic, pelsparitic, biomicritic, oncolitic and in-
traclastic limestones with LLH stromatolites, pellets, pseudoooids, oncoids, gas-
tropods, benthic foraminifera as well as numerous fenestrae, desiccation cracks and
erosion surfaces. Among clasts are most common intraclasts, pellets and pseudoooids.
For the lower part of the Valanginian stratigraphie sequence an alternation of micro-
crystalline dolomites and more or less dolomitized limestones is characteristic. At so-
me places a rhythmic alternation of light gray early-diagenetic and dark gray to bro-
wnish gray, coarse-grained, bituminous late-diagenetic dolomite can be observed.
Strata rich in oncoids occur in the upper part of the succession. Microfauna and mi-
croflora are rare. Most frequent and numerous are textularians, favreinas and clypei-
nas. In the described carbonate sediments the mosaic cement B and fibrous early dia-
genetic cement A are most common. Granular cements are coarser in birdseyes fil-
lings and finer in packstone and grainstone carbonates. According to structural and
textural properties the Valanginian carbonate rocks were formed in shallow lagoon
as well as subtidal, intertidal and supratidal environments.
Hauterivian
The Hauterivian beds are composed of thick-bedded (40-100 cm), medium gray
and light gray limestones. In the lower part of the Hauterivian lithological column
extremely thick-bedded (75-200 cm) limestones occur. According to texture the li-
mestones belong to micrites, pelsparites, biopelmicrites, biointrasparites, oosparites,
pseudooosparites, oncolites and stromatolites. In the Hauterivian stratigraphie se-
quence limestones strongly prevail. Dolomites and carbonate clastic rocks are rare.
In the lowermost part of the Hauterivian sedimentary succession stromatolites con-
taining gastropods, ostracods, foraminifera, intraclasts and pellets are quite abun-
dant.
Neocomian
On the Jurassic/Lower Cretaceous boundary some parts of the studied area were
subjected to tectonic movements as consequence of the Late Kimmerian orogenetic
phase, resulting in the uplifting and rupturing of particular parts of the sea bottom.
The newly formed land gave the material for heterogeneous limestone, dolomite, and
limestone-dolomite sedimentary breccia intercalated with dolomite and limestone.
These beds lie erosionally, and slightly discordantly upon the Upper Malm lime-
stone and dolomite succession. At some places there are no traces of orogenetic acti-
vity; intensified epeirogenic movements can be followed resulting in more intensive
sinking of the sea bottom and continuous sedimentation of the Lower Cretaceous se-
quence of limestones and dolomites.
The Neocomian beds are composed of heterogeneous limestone-dolomite breccia
which contains fragments of various Jurassic limestones and dolomites, and in the
Prezidanski Berišček area fragments of chert, too. Consequently, two types of Neoco-
mian breccia can be found: carbonate breccia and carbonate-chert breccia.
158_Stevo Dozet & Ljudmila Šribar
The carbonate-chert breccia is composed of angular and subangular fragments of
gray, medium gray and dark gray micrite, biomicrite, biosparite and rarely oosparite,
further on, fragments of dark gray medium- and coarse-grained bituminous dolomite
as well as 1 cm to 5 cm angular dark gray chert fragments. Carbonate and chert fra-
gments from 5 cm to 30 cm are rare. Sporadically occur in the breccia mollusc fra-
gments. Some fragments contain the Upper Malm microfossils. The described fra-
gments are bounded together with basal and pore cement. The breccia is massive to
poorly stratified. Contacts among beds are not clear. Occasionally, intercalations of
medium gray, gray, dark gray and grayish black oomicritic limestone, dolomitized
micritic limestone and coarse-grained dolomite occur in the carbonate-chert breccia.
Since the breccia contains fragments with the Upper Malm fauna, and it is overlain
by the limestones containing the Barremian-Aptian microfossil association, the brec-
cia corresponds to Neocomian (Savie, 1973; Savie & Dozet, 1985). The thic-
kness of the Neocomian beds ranges from 100 m to 120 m.
Barremian
Two developments of the Barremian beds can be distinguished in the study area:
the limestone and the limestone-dolomitic development. The limestone development
includes medium- and thick-bedded as well as thin-bedded and platy medium gray,
gray, dark gray, blackish gray and black, more or less bituminous micrites, pelmicri-
tes, pelsparites, biointrasparites, biosparites, stromatolites, rarely intraformational
breccias and conglomerates. Among biomicrites and biosparites foraminiferal and
occasionally algal limestones predominate. Rhythmic sedimentation of enumerated
limestones is very common. Numerous intertidal oscillations, shallowings and emer-
sions can be observed in the considered stratigraphie sequence. The emersions were
accompanied by interruptions of sedimentation, weak erosion and carbonate breccias
of various origin. Also characteristic is a rhythmic alternation of light-coloured early
diagenetic and dark late diagenetic dolomites. The late diagenetic dolomites mostly
originated by dolomitization of micrites, pelsparites, pelmicrites, intrasparites, and
especially oncolites and stromatolites. Complete and selective dolomitization are pre-
sent. Consequently, all types from limestone to dolomite can be seen in the Barremian
sedimentary succession. Late diagenetic dolomite occurs in the form of thick beds,
lenses and irregular patches or bodies. They consist of more or less coarse-grained
and bituminous dolomite.
Aptian
Lower Aptian-Bedoulian. Upon the Barremian sediments lie conformably bedded
and platy dark gray and grayish black, rarely gray and light gray micritic, biomicri-
tic, intramicritic, biointrasparitic more or less bituminous limestones. At some places
miliolids and salpingoporellas are accumulated in such quantities that they are rock-
building. Bedoulian beds build the outer parts of Kočevje and Požar synclines and
are exposed also in the extremely southwest part of the Kolpa area. For the Lower
Cretaceous are especially characteristic the lagoonal and back reef sediments consi-
sting of micrites, biomicrites, biosparites, oncolites and intrasparites. These sedi-
ments predominantly originated in a shallow and calm restricted marine environ-
Lower Cretaceous Shallow-Marine Sedimentation and Biota_ 7
ment with numerous green algae (Dasycladacea, Codiaceae), foraminifera (miliolids,
orbitolinids) and ostracods. In some layers moluscs (small requienids and gastropods)
occur Relatively common with gastropods, orbitolinids and Bacinella are incrusted
oncolites. Furthermore, for the Lower Aptian succession a rhythmic alternation of
micrites, biomicrites and oncolites is characteristic too.
The most characteristic for the lower part of the succession are the so-called Lo-
wer Orbitolina limestones, orbitolinid biomicrites and biosparites respectively, invol-
ving gastropods, miliolids and salpingoporellas. Laminated sediments are rare. Inter-
layers of limestone breccia and dark gray bituminous dolomite are also pretty rare.
Consequently, the Lower Cretaceous sediments were prevalently formed in lagoonal,
subtidal and other shallow marine environments.
Coral-rudist patch reefs. Lagoonal, subtidal and other shallow marine micrites, bi-
omicrites and oncolites pass at some places into reef facies that consists of reef-buil-
ding macroorganisms such as corals, bryozoans, primitive rudistids, gastropods,
echinoids as well as algae and foraminifera. Coral-rudist reef limestones with orbito-
linas in the Kočevje area were found earlier by Uršič (1933). In the coral limestone
at Spodnje Ložine and at Koblerski Hrib Uršič mentioned 5 coral species, namely:
Isastraea hoernesi, Lithoraea vaughani, Phyllosmilia transiens, Montlivaltia lamx,
Cyclotites nummulus in C. hemisphaerica. Coral-rudist features of patch-reef type
were discovered east of Željne and southeast of Škodovnik in the Kočevje area (Dozet,
1983). T u r n Š e k et al. (1992) examined the coral-rudist reef development of Slo-
venski vrh probably corresponding to the white coral limestone and white yellow
chamid limestone of II. horizon quoted by Uršič (1933). The coral-rudist reef on
Slovenski vrh belongs to a patch reef of the inner part of the Dinaric carbonate plat-
form. In the lower part of the reef predominate rudists of Caprina-Praecaprina and
Offneria type, and corals of the type Cyathophora-Actinaraea-Microsolena. In the
upper part of the Aptian-Albian reef the rudist species Ichthyosarcolites and corals
Procladocora-Strotogyra type (T u r n š e k et al., 1992) occur
T u r n š e k et al. (1992) determined the following corals and rudists in the rock
samples collected at the top of Slovenski vrh:
Corals: Cyathophora pygmaea Volz, Peplosmilia fromenteli Angelis d'Ossat, Pro-
cladocora kocevjensis n. sp., Calamophylliopsis fotisalensis (Bendukidze), Strotogyra
augusti n. sp., Microsolena distefanoi (Prever) and Actinaraea tenuis Morycowa.
Rudists: Ichthyosarcolites monocarinatu^ Slišković, Monopleura sp., and Offneria sp.
According to its shape, extension and fauna the coral-rudist reef at Željne belongs
to a relatively small patch reef originated in the inner part of the Dinaric carbonate
platform. In the patch reef area a vertical and lateral differentiation of fauna can be
observed. In the lower part of the patch reef rudistids of the Requenia and Toucasia
type predominate, whereas in the upper part corals occur. Rudistid biostromes, coral
bioherms and coral detritus point at a patch reef as well as periodically open and
wavy shallow marine environment. Rudists, corals, bryozoans as well as echinoderms
and molluscs indicate open shoals and smaller isolated patch reefs populated with
the enumerated organisms. To all appearance patch reefs were extended in the Apti-
an and Albian in the inner parts of the Dinaric carbonate platform.
In the coral patch reefs area the following microfossils have been determined: Pa-
lorbitolina lenticularis (Blumenbach), Praeorbitolina wienandsi Schroeder, P. cormyi
Schroeder, Orbitolina (Mesorbitolina) lotzei Schroeder, Orbitolina (Mesorbitolina) te-
xana Roemer, Neotrocholina friburgensis Guillaume & Reichel, Debarina hahoune-
rensis Fourcade et al., Spiroloculina cretacea Reuss, Bacinella irregularis Radoičič,
160_Stevo Dozet & Ljudmila Šribar
Paleodictyoconus sp., Nezzazata sp., Trocholina sp., Sabaudia sp., Praechrysalidina
sp., Miliolidae, Ophthalmidiidae and Textulariidae. According to the enumerated mi-
crofauna and microflora the patch reefs of the study area belong to the Aptian-Lower
Albian period.
Upper Aptian-Gargasian. The Upper Aptian corresponds to the interval between
the Lower and Upper Orbitolina limestones. Relatively numerous erosion surfaces
and layers of intraformational breccias at the end of the Lower Aptian indicate in-
tensified shallowing of the study area. The Upper Aptian beds are found on Požar-
je, Kočevsko pogorje, to the east of Željne and in the extremely nordeastern part of
the Delnice map sheet. However, the Upper Aptian succession does not differ essen-
tially from the Lower Aptian one. Shallow marine subtidal and lagoonal fades of
micrites, biomicrites, rhythmically alternating with foraminiferal and mollusc bio-
intrasparites and biosparites as well as patch reefs and oncolites represent the main
characteristics of the Upper Aptian sedimentation. The examined geological inter-
val is relatively rich as in diversity of fades as in fossils. In the patch reefs rudi-
stids and corals form the framework structure. To the structure of the patch reefs
contribute their part bryozoans, codiaceans and other algae, molluscs and echino-
derms. The fades surrounding the patch reefs consists of biosparites, biointraspari-
tes and biosparrudites (packstones, grainstones and rudstones). In the lagoon
rhythmic micrites, pelmicrites as well as miliolid, Salpinogoporella, dasycladacean
and foraminiferal biopelmicrites and biomicrites (wackestone, packstone) occur in-
dicating normal shallow marine conditions in an open lagoonal inner shelf environ-
ment.
Albian
Lower Albian. The limestones with Salpingoporella dinarica are overlain by lime-
stones containing numerous orbitolinids. Orbitolinas in the limestone are so numero-
us that they are rock-building. These sediments are known under the name of the up-
per Orbitolina limestones (Velie, 1977; Velie & Sokač, 1978a, b) correspon-
ding biostratigraphically to the Lower Albian. The sedimentary succession consists
of bedded and platy, dark gray, gray and dark brownish gray, bituminous micrites,
pelmicrites, biomicrites and biosparites. Among biomicritic and biospari tic limesto-
nes predominate the orbitolinid and miliolid ones. Oncolites and requienid lumachel-
les are present but are relatively rare. Lumachelles with gastropods also occur in this
interval of the Lower Cretaceous sequence. The limestones usually contain some or-
ganic admixture being therefore brownish.
Upper Albian. At the end of the Lower Albian a shallowing tendency (lagoon-
shallow subtidal-intertidal-supratidal) occurred. At the beginning of that period a
rhythmic sedimentation of stromatolites and intraformational breccia predominated.
In fact, the Upper Albian succession chiefly consists of stratified or platy dark gray
micritic, pelmicritic, biomicritic and biosparitic limestones. Lagoonal and subtidal
sedimentation (micrite, biomicrite) also prevails in the upper part of the Upper Albi-
an stratigraphie sequence. Pretty common are the miliolid biomicrites. Lumachelles
with small requienids are still present. In the uppermost part of the succession coar-
se-grained dark gray and brownish gray bituminous dolomites and intrasparrudites
predominate. The dolomites were formed by the late dolomitization of micrites, onco-
lites, intrasparrudites and stromatolites.
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 161
In the study area the transition from the Lower to the Upper Cretaceous beds is
not clear either from paleontological or lithological point of view. This is a consequence
and influence of the orogenetic movements of the Austrian tectonic phase (Dozet,
1989). On the boundary between the Lower and the Upper Cretaceous occurs a some
hundred metres thick transitional succession of alternating breccia, dolomite and li-
mestone. The boundary between the Lower and the Upper Cretaceous passes within
this sequence.
Biostratigraphy
On the basis of characteristic lithofacies and biofacies as well as their superpositi-
on the shallow marine Lower Cretaceous stratigraphie sequence in the area between
Logatec and Krka and Kolpa Rivers (Fig. 1) consists of the following characteristic
Fig. 1. Location sketch map of investigated area
SI. 1. Položajna karta raziskanega ozemlja
lithofacies (Fig. 2): carbonate and carbonate-chert breccias, fenestral, stromatolitic
and laminated limestones and dolomites, late-diagenetic dolomites, oncolitic, biocla-
stic, micritic, intraclastic, patch-reef and coquina limestones. The enumerated se-
dimentaiy carbonate rocks contain rich microfossil associations which are very im-
162
Stevo Dozet & Ljudmila Šribar
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 163
portant, useful and characteristic for biozonation of the Lower Cretaceous beds.
From the biostratigraphic point of view the Lower Cretaceous sedimentary successi-
on has been divided by microfossils into five cenozones and four subzones (Fig. 3). In
the study area the Lower Cretaceous microfossils belong to two main'groups, namely:
Fig. 3. Biostratigraphic subdivision of the Lower Cretaceous beds
in southeastern Slovenia
SI. 3. Biostratigrafska razčlenitev spodnjekrednih plasti južno-
vzhodne Slovenije
calcareous algae Dasycladacea and benthic foraminifera Orbitolina. Algae are nume-
rous and important in Berriasian, Valanginian, Hauterivian, Barremian, and Aptian;
on the other hand, foraminifera predominate in the Lower Aptian and Albian.
164_Stevo Dozet & Ljudmila Šribar
Cenozone Clypeina ? solkani
This cenozone is denominated according to the alga Clypeina ? solkani Conrad &
Radoičić (Plate 3) which appears at the beginning of Berriasian (Strohmenger
& D o z e t, 1991) and expanding in Valanginian and Hauterivian. The lower boun-
dary of this biozone is represented by the appearance of the alga Clypeina ? solkani,
whereas the upper one by the total disappearance of the mentioned alga. In the study
area the Jurassic sedimentary succession passes gradually into the Lower Cretaceous
one. In the carbonate sediments which according to their stratigraphie position be-
long to Berriasian no diagnostic fossils occur. Due to very specific conditions of sedi-
mentation microfossils are rare and biostratigraphically non significant. Numerous
and in some way important are only the species Favreina salevensis Paréjas and Sal-
pingoporella annulata Carozzi (Plate 1) that are accompanied by numerous small fo-
raminifera, especially Textulariidae, Verneuilinidae, Ophthalmidiidae and Milioli-
dae. Beside species Clypeina and Salpingoporella the alga Thaumatoporella parvove-
siculifera (Raineri) as well as Charophyta oogonia (Plate 1) also occur. Among fora-
minifera also appears the species Pseudocyclammina lituus (Yokoyama), which is
common as in the Upper Malm sediments also through the whole Lower Cretaceous
stratigraphie sequence, up to Albian. Among other fossil groups stromatoporoids,
ostracods and gastropods (nerineids) have been found. The described association of
microfossils is ranged into the subzone Favreina salevensis-Salpingoporella annula-
ta. As already said, there are no real Berriasian diagnostic fossils. However, due to
their maximum abundance in this time interval, the Favreina salevensis and Salpin-
goporella annulata can be considered and used as Berriasian characteristic fossils.
In Valanginian the sea became somewhat deeper and several characteristic species
of algae and foraminifera occur The most important and relatively abundat was spe-
cies Clypeina ? solkani Conrad & Radoičić that gave the name to the oldest Lower
Cretaceous cenozone. In the middle part of the cenozone, which corresponds to the
Valanginian stage, rare sections of the species Cuneolina tenuis Velie & Gušić have
been found. Beside the guide alga Clypeina ? solkani the Valanginian sediments also
contain associations of fossils composed of salpingoporellas, cuneolinas, thaumato-
porellas, ostracods and the algae Epimastopora ? cekici. Microfossils Cuneolina tenu-
is and Epimastopora ? cekici Radoičić have their maximum abundance in Valangini-
an but can also be present in the Hauterivian. Some Valanginian characteristic fossils
are accompanied by species with the stratigraphie range from Jurassic to Barremian
(Salpingoporella annulata Carozzi). The alga Clypeina ? solkani Conrad & Radoičić
has its maximum abundance in Hauterivian.
Lithologically, the Valanginian-Hauterivian passage is designated by intensified
intertidal oscillations and rhythmic sedimentation of pelmicrites, micrites, biomicri-
tes, oncolites, stromatolites, fenestral carbonates as well as intrasparites and bio-
intrasparites.
In the Hauterivian part of the cenozone Clypeina ? solkani the foraminifera Or-
bitolinopsis capuensis (De Castro) appear. Beside the above quoted characteristic
microfossils the Hauterivian involves some other microfossils with wider stratigra-
phie range, such as salpingoporellas, sabaudias, miliolids, ophthalmidiids and tha-
umatoporellas. The described Hauterivian association belongs to the subzone Epi-
mastopora ? cekici + Orbitolinopsis capuensis. In the upper part of the Clypeina ?
solkani cenozone still appear numerous foraminifera Cuneolina ex. gr. laurentii-
camposaurii Sartoni & Crescenti, Debarina hahounerensis Fourcade et al., Pseudo-
Lower Cretaceous Shallow-Marine Sedimentation and Biota_ 165
textulariella ? scarsellai (De Castro), Glomospira sp., Miliolidae, Ophthalmidiidae
and Textulariidae.
Cenozone Salpingoporella muehlbergii
The cenozone Salpingoporella muehlbergii, which is relatively poor in diagnostic
fossils, lies between the cenozones Clypeina ? solkani and Salpingoporella dinarica,
which are well defined by diagnostic fossils. For the second Lower Cretaceous ceno-
zone are characteristic blue-green algae Dasycladaceae, among which Salpingoporel-
la muehlbergii (Plate 4) is the most extended: for this reason, the name of the second
Lower Cretaceous cenozone, which chronostratigraphically includes the Barremian
stage, is given according to this algae. Otherwise, the microfossil association of the
considered cenozone is relatively rich involving beside salpingoporellas /Salpingopo-
rella muehlbergii (Lorenz), Salpingoporella melitae (Radoičić), Salpingoporella sp./
also algae Thaumatoporella parvovesiculifera (Raineri), Codiaceae, Cyanophyceae as
well as the following foraminfera: Cuneolina ex. gr. laurentii camposaurii Sartoni &
Crescenti, Debarina hahounerensis Fourcade et al., Nezzazata simplex Omara, Saba-
udia minuta (Hofker), Pseudotextulariella ? scarsellai (De Castro), Glomospira sp.,
Nezzazata sp., Orbitolinidae, Miliolidae, Lituolidae, Ophthalmidiidae and Textularii-
dae. Beside foraminifera and algae in the Barremian carbonate rocks ostracods, echi-
noderms and molluscs occur, too. In spite of lack of real diagnostic fossils the boun-
daries of this cenozone are clear; the lower boundary passes through the point of di-
sappearance of characteristic fossils of the cenozone Clypeina ? solkani, whereas the
upper boundary is marked by the appereance of the algae Salpingoporella dinarica
and the foraminifera Palorbitolina lenticularis (Blumenbach).
Cenozone Salpingoporella dinarica
This cenozone comprises the whole Aptian sedimentary succession together with
the fossil contents. It is named by the characteristic alga Salpingoporella dinarica
Radoičić (Plate 5) which is very common especially in the upper part of the Aptian
stratigraphie sequence. In the lower part of the Aptian succession numerous orbitoli-
nids can be seen. Owing to their small vertical stratigraphie range the orbitolinids
are very usefull for detailed subdivision and biozonation. On the basis of orbitolinids
it is possible to subdivide the Aptian stratigraphie sequence of the study area into the
Lower Aptian (Bedoulian) and the Upper Aptian (Gargasian). The lower part of the
cenozone is designated as the subzone Palorbitolina lenticularis (Blumenbach). From
the lithostratigraphical point of view the lower part of the cenozone corresponds to
the lower Orbitolina limestones. Beside the characteristic Palorbitolina lenticularis
(Plate 6/1-2) and algae Salpingoporella dinarica (rather rare in the lower part of the
Aptian succession), numerous other foraminifera and algae occur:
Foraminirefa: Praeorbitolina cormyi Schroeder, P. wienandsi Schroeder, Trocholi-
na friburgensis Guillaume & Raichell, Debarina hahounerensis Fourcade et al., Saba-
udia minuta (Hofker), S. auruncensis (Chiocchini & Di Napoli Alliata), Pseudotextu-
lariella ? scarsellai (De Castro), Nezzazata simplex Omara, Ovalvelina cf. reichelli De
Castro, Cuneolina sp., Nummoloculina sp., Glomospira sp., Biokovinidae, Miliolidae,
Textulariidae and Ophtalmidiidae.
166_Stevo Dozet & Ljudmila Šribar
Algae: Bacinella irregularis Radoičić (Plate 7/1-2), Thaumatoporella parvovesicu-
lifera (Raineri), Lithocodium aggregatum Elliot and Salpingoporella sp. Moreover,
numerous rudists and corals settled the small Aptian patch reefs. Orbitolinids, milio-
lids, salpingoporellas and requienids, being often rock-building, reach in Aptian the-
ir maximum abundance. In fact, the Upper Aptian corresponds to the interval betwe-
en the lower and upper Orbitolina limestones characterized by maximum abundance
of the species Salpingoporella dinarica. There are no proper Gargasian diagnostic
fossils. However, due to maximum abundance the algae Salpingoporella dinarica can
be considered as the Upper Aptian characteristic fossil. On the boundary between the
Lower and Upper Albian the species Sabaudia minuta (Plate 7/4) and Pseudotextula-
riella ? scarsellai (Plate 7/3) disappeared.
Cenozone Orbitolina (Mesorbitolina) ex gr. texana
Upon the beds with the alga Salpingoporella dinarica lie conformly the 80 metres
thick upper Orbitolina limestones which are built of numerous orbitolinas. Their
stratigraphie range corresponds to the Lower Albian. Accordingly, the cenozone Or-
bitolina (M.) ex gr. texana begins with the extinction of Salpingoporella dinarica and
with the first appearance of the species O. (M) texana (Plate 6/3-4) and ends with the
disappearance of the latter mentioned foraminifer Thus, the cenozone is characteri-
zed by mesorbitolinas and by numerous microorganisms with a wider stratigraphie
range, such as: Sabaudia minuta (Hofker), S. auruncensis (Chiocchini & Di Napoli
Alliata), Vulvulammina picardi Henson, Pseudotextullariella ? scarsellai (De Castro),
Debarina hahounerensis Fourcade et al., Bacinella sp. and Miliolidae. Orbitolinids
were rock-building. They lived in a calm lagoonal and shallow marine environment.
Cenozone "Valdanchella" dercourti
In the uppermost part of the Lower Cretaceous stratigraphie sequence primitive
orbitolinids occur. Among them the diagnostic species "Valdanchella" dercourti (Pla-
te 8/1) is relatively well extended. Beside the diagnostic primitive orbitolinas nume-
rous other foraminifera can be seen, namely: Cuneolina ex gr. pavonia parva Henson
C. ex gr. laurentii-camposaurii Sartoni & Crescenti, Nummoloculina heimi Bonet
(Plate 8/2), Nezzazata simplex Omara, Debarina hahounerensis Fourcade et al., Val-
vulammina picardi Henson (Plate 8/3), Nummoloculina. sp., as well as numerous Mi-
liolidae, Ophthalmidiidae and orbitolinids. Algae are rare in the Upper Albian beds.
Only remains of Thaumatoporella parvovesiculifera (Raineri), Salpingoporella turgi-
da (Radoičić) (Plate 8/4) and Salpingoporella cf. hasi Conrad et al. can be found.
Discussion and Interpretation
Several sections of the Lower Cretaceous beds in the area between Logatec and
the rivers Krka and Kolpa have been studied. Our data are based on field observati-
ons as well as thin-section analysis. Detailed section study and regional correlation
of the Lower Cretaceous stratigraphie sequences indicate a high similarity of mine-
ralogical, textural, structural and environmental characteristics as well as high simi-
Lower Cretaceous Shallow-Marine Sedimentation and Biota_ 15
larity of associations of fossils throughout the whole study area. Generally speaking,
sedimentological and paleontological properties suggest that the Lower Cretaceous
carbonates were formed in the inner part of the Dinaric carbonate platform in vario-
us shallow-marine depositional environments, namely: littoral, lagoons, restricted
shoals, as well as reef. Eustatic, intertidal and tectonic movements caused a differen-
tiation of the carbonate platform (various depositional environments), lateral and
vertical changes, different thickness of sediments and rhythmic sedimentation. Seve-
ral developments of the Lower Cretaceous beds can be recognized in the study area.
A poor faunal diversity i.e. a low number of species, stromatolites, birdseyes, nume-
rous local erosion surfaces, common occurrences of marine and meteoric cements, do-
lomitization, occurrences of karstification indicate a short lasting supratidal envi-
ronment during Berriasian, Valanginian and Hauterivian. Locally, the dry land sta-
yed through the whole Valanginian and Hauterivian. The shallow marine conditions
became predominant at the beginning of the Lower Barremian. In the Upper Barre-
mian two main types of sediments can be distinguished: (1) - subtidal to lagoonal mi-
crites, biomicrites and oncolites, and (2) - intertidal to supratidal intramicrites, in-
trasparites, stromatolites and intraformational breccias, dolomites. Normal marine
conditions, subtidal and lagoonal environment respectively, characterized by high fa-
unal and floral diversity were established at the beginning of Aptian. In the middle
and at the end of Aptian there were tendencies of eustatic and intertidal oscillations
as well as slight tectonic movements, which were manifested by rhythmic alternation
of biomicrites, biosparites, intramicrites, intrasparites, biointrasparites, stromatoli-
tes and intraformational breccias. Subtidal to lagoonal regime with several small
patch reefs settled by corals, requienids and algae, back reefs and shoals was domi-
nant in the Lower Albian and Aptian. The Upper Albian is characterized by frequent
changes of sedimentation and depositional environments, from subtidal and lagoonal
environment rich in microfossils to intertidal ones poor in fauna and flora. In that ti-
me late diagenetic dolomites were pretty extended. The described carbonate rocks
are often diagenetically changed.
In the Aptian and Lower Albian the coral-rudistid reefs in the Željne, Škodovnik,
Spodnje Ložine, Koblerski hrib and Slovenski Vrh area belong to patch reefs origina-
ting in a central part of the lagoon. Vertical differentiation can be observed on the
mentioned patch reefs. In the lower part of the reef rudists Monopleura-Praecaprina-
Ojfneria type and corals of massive bulbous and lamellar Cyathophora-Actinaraea-
Microsolena type predominate (Turnšek et al., 1992). Colonies are small and rare
indicating a low rate water energy. In the upper part of the reef the rudist Ichthyosar-
colites and corals Procladocora-Strotogyra are widespread indicating a higher water
energy environment. In the uppermost part usually the codiaceans Lithocodium oc-
cur. Coral-rudist reefs appear to be present but not extremely common in the Aptian
and the Lower Albian beds.
Acknowledgement
The authors gratefully acknowledge Dr. Rajka Radoičić for valuable suggestions.
Appreciation is expressed to Prof. Dr. Stanko Buser and Asst. Prof. Bojan Ogorelec,
who provide a very helpfull review of the manuscript and to Prof. Dr. Simon Pire,
who reviewed the English text. For technical assistance in drafting and typing we
would like to thank Ms. Metka Karer and Ms. Marjeta Oman.
168_Stevo Dozet & Ljudmila Šribar
Spodnjekredna plitvomorska sedimentacija, favna in flora na Dinarski
karbonatni platformi med Logatcem, Krko in Kolpo
Sklep
V južnovzhodni Sloveniji med Logatcem, Krko in Kolpo so se v plitvem spodnje-
krednem morju odlagale debele plasti apnencev in dolomitov. Na podlagi favne in
flore ter stratigrafske lege so na obravnavanem ozemlju ugotovljene vse spodnjekre-
dne stopnje, in sicer: berriasij, valanginij, hauterivij, barremij, aptij in albij. Meja
med krednim in jurskim sistemom je v tem delu Dinarske karbonatne platforme lito-
loško jasna samo tam, kjer sta razvita bazalni konglomerat in breča. Tu gre za erozij-
sko, deloma tektonsko-erozijsko diskordantno mejo, ki označuje prekinitev v sedi-
mentaciji in tektonske premike na meji med juro in kredo. Drugod je kontakt med
jurskimi in krednimi plastmi normalen, brez pomembnejših sprememb v sedimenta-
ciji. Konkordantno na zgomjemalmskih apnencih leže berriasijski, pretežno lamini-
rani in stromatolitni apnenci in dolomiti s pogostnimi izsušitvenimi razpokami in po-
rami, zapolnjenimi z mikritom, peleti, intraklasti ali z organskim detritusom. Berria-
sij ske plasti so revne s fosili in praviloma bolj ali manj dolomitizirane. Litološka se-
stava ter struktura in tekstura obravnavanih sedimentov kažejo, da so berriasijske
plasti nastale pretežno v nadplimskem in medplimskem okolju. To dokazujejo pogo-
stni laminirani karbonatni sedimenti z izsušitvenimi razpokami, stromatoliti, zgo-
dnjediagenetski dolomiti, gravitacijski cement in nadplimski konglomerat. Valangi-
nijsko sedimentno zaporedje sestoji iz plastnatih mikritnih, pelmikritnih, pelspari-
tnih, biomikritnih, onkolitnih in intraklastičnih apnencev. Pogoji za življenje so bili v
berriasiju, valanginiju in hauteriviju dokaj neugodni, kar dokazujeta pičla favna in
flora v teh sedimentih. Med mikrofosili se v teh plasteh pojavljajo miliolide, tekstula-
rije, favreine in klipeine. Valanginij ski sedimenti imajo v glavnem enolično strukturo
brez notranjih ali zunanjih tekstur. Ponekod v njih opazujemo vodoravno laminira-
nost ali redke stromatolite. Pretežni del sedimentov valanginijskega zaporedja je
nastajal v plitvi in mimi vodi zaprtega šelfa in lagun. Hauterivijske plasti so zgrajene
v glavnem iz debeloplastnatih mikritnih pelsparitnih, biopelmikritnih, onkolitnih,
biointrasparitnih, oosparitnih, pseudoosparitnih in stromatolitnih apnencev. Pretežni
del hauterivijskih sedimentov se je odlagal v podplimskem in lagunskem okolju. V
barremijskem sedimentnem zaporedju ločimo v splošnem dva razvoja, in sicer apnen-
čevo-dolomitni in apnenčev razvoj. V strukturnem pogledu prevladujejo med apnenci
mikriti, pelmikriti, pelmikrospariti in biopelspariti. Pogosto je ritmično menjavanje
kamenin. Menjavajo se zlasti mikriti, pelmikriti in biopelmikriti, ponekod intrami-
kriti, intraspariti biointraspariti, drugod mikriti, pelmikriti, stromatoliti, medplim-
ske breče ali zgodnje- in poznodiagenetski dolomit. Pretežni del barremijskih sedi-
mentov se je gradil v podplimskem in lagunskem okolju. Drugi barremijski sedimenti
so nastajali znotraj plitvega karbonatnega šelfa, večkrat v razgibani vodi.
Močni epirogenetski premiki ob pomoči šibkih orogenetskih sil konec barremij a so
povzročili dviganje morskega dna. Morje je postalo plitkejše, ponekod je nastalo ko-
pno. Na njem je nastopala erozija. Sledila je kratkotrajna transgresija, rezultat le-te
pa so bile tanj še plasti apnenčeve breče, s katerimi se je ponekod na raziskanem ozem-
lju pričenjalo aptijsko zaporedje sedimentov. Toplo, čisto, mimo, primemo slano in od
časa do časa bolj ali manj razÌDurkano morje je bilo ugodno za naselitev dasikladacej
in številnih bentonskih organizmov, med katerimi so po številu prednjačile miliolide.
V obdobjih razburkanega morja so živele orbitoline. Na robu karbonatne platforme so
se ponekod oblikovali koralni grebeni in biostrome z moluski. Korale so naseljevale
obrobja plošč. Koralno-radistni grebeni so pripadali "patch" grebenom. Nastajali so
Spodnjekredna plitvomorska sedimentaci]a, favna in flora ..._
znotraj karbonatne platforme. Po mikrofavni sodeč, so se koralno-rudistni grebeni
ohranili še v albiju. Sicer pa se je aptijsko albijska sedimentacija dogajala večidel v
lagunskem in podplimskem okolju. V mimi in dokaj plitvi vodi so se odlagali mikritni,
pelmikritni, biopelmikritni in tanko laminirani bolj ali manj bituminozni apnenci. Na
občasno zelo plivo okolje kažejo tudi lumakele z drobnimi rekvienidami, katerih lupi-
ne so se po izumrtju teh organizmov kopičile in odlagale v plasteh.
Spodnjealbijski apnenci so nastajali deloma v mimi vodi podplimskega pasu ali la-
gun, večidel pa na obsežni karbonatni platformi, ki je imela pogosto stik z odptim mor-
jem. Odpto morje in voda s povečano energijo sta bolj ali manj stalno spirala in
prezračevala dno nekoliko poglobljenega šelfa, kar je bilo ugodno za rast številnih or-
ganizmov in za nastanek biosparitov, biointrasparitov in intraklastičnih sedimentov.
Take razmere so bile ugodne zlasti za življenje in bogat razvoj rekvienid in drugih mo-
luskov, ki so ustvarjali obsežne trate na bolj ali manj ravnem dnu. Proti koncu zgornje-
ga albija so se fizikalno-kemični pogoji v albijskem morju pričeli močno spreminjati.
K temu je največ pripomogla vedno bolj prisotna in naraščajoča tektonska dejavnost,
ki je povzročila spremembe v globini vode. Močno so se spremenile tudi okoliščine za
življenje organizmov. Poglobljeni self, v katerem so nastajali zgomjealbijski sedimenti,
je postajal vse bolj plitev. Mnogi organizmi niso prenesli pogostnih naglih sprememb in
so začeli izumirati. To velja zlasti za številne rodove foraminifer. Pojavile so se nove vr-
ste, ki so bile sposobne kljubovati vsem spremembam globine in energije vode. Tako so
se na začetku zgornje krede v plitvi in zelo plitvi razgibani vodi močno razmnožili rudi-
sti, ki so ustvarjali obsežne morske trate in pogosto celo manjše grebene.
Zahvala
Avtorja se zahvaljujeva dr. Rajki Radoičič za koristne nasvete. Za kritično oceno
rokopisa, ki je pripomogla k njegovi izboljšavi, se zahvaljujeva uredniku revije prof.
dr. Stanku Buserju in doc. dr. Bojanu Ogorelcu. Zahvala velja tudi prof. dr. Simonu
Pircu za pregled angleškega besedila ter sodelavkama Meti Karer in Marjeti Oman za
tehnično pripravo članka.
References
B u s e r, S. 1968: The development of Jurassic strata in the Outer Dinarides of Slovenia
(orig. in Slov.). - First Coll. Geol. Dinaric Alps. Geol. Survey and Geol. Society of Slovenia, 1,
59-67, Ljubljana.
B u s e r, S. 1974: Tolmač k Osnovni geološki karti list Ribnica 1 : 100 000. - Zvezni geološki
zavod, 60 p., Beograd.
B u s e r, S. 1989: Development of the Dinaric and Julian Carbonate platforms and of the in-
termediate Slovenian basin (NW Yugoslavia). - Mem. Soc. Geol. It., 40 (1987),
313-320, Rome.
Dozet, S. 1983: Tolmač za list Delnice. Osnovna geološka karta SFRJ (int. repport). - Geo-
loški zavod Ljubljana - IGGG, 109 p., Ljubljana.
Dozet, S. 1989: Razvoj mezozojskih plasti na Kočevskem in v okolici. Disertacija. -Geolo-
ški zavod - IGGG, 187 p., Ljubljana.
Dozet, S. 1990: Biostratigraphic subdivision of the Jurassic and Lower Cretaceous beds in
Kočevje and Gorski Kotar area (orig. in Slov.). - Rud.- met. zbornik, 37, 1, 3-18, Ljubljana.
Dozet, S. & Šribar, L. 1991: Lower Cretaceous beds on the Delnice Sheet (orig. in
Slov). - Rud.-met. zbornik, 38, 1-2, 161-190, Ljubljana.
Dunham, R. J. 1962: Classification of carbonate rocks according to depositional texture,
- In: W. E. H a m (ed.), Classification of carbonate rocks. - AAPG Memoir 1, 108-121, Tulsa.
Farinacci & Radoičić, R. 1964: Correlazione fra serie giuresi e cretacee dell' Ap-
pennino centrale e delle Dinaridi esteme. - Ric. Sci., 34, serie 2, parte II A, voi. 7, n.2., 269-300,
iloma.
170_Stevo Dozet & Ljudmila Šribar
Folk, R. 1959: Practical pétrographie classifications of limestones. - Bull. Americ. Assoc.
Petrol. Geol., 43/i, 2-38, Tulsa.
Orehe k, S. & Ogorelec, B. 1979: Sedimentologie features of the Jurassic and Creta-
ceous carbonate rocks of Trnovski gozd (orig. in Slov). - Geol. Vjesnik, 32, 185-192, Zagreb.
Orehe k, S. & Ogorelec, B. 1981: Correlation of microfacial and geochemical characte-
ristics of Jurassic and Cretaceous rocks of the southern carbonate platform in Slovenia (orig. in
Serbo-Croat.). - Glas, republ. zavod. zašt. prir - Prir muzeja (Titograd), 14, 161-181, Titograd.
P 1 e n i č a r, M. 1970: Tolmač za list Postojna. Osnovna geološka karta SFRJ 1 : 100 000. -
Zvezni geološki zavod, 62 p., Beograd.
P 1 e n i č a r, M. & Šribar, L. 1983: Cretaceous beds between Kočevje and Krka (orig. in
Slov). - Geol. zbornik, 4, 47-79, Ljubljana.
Radoičić, R. 1960: Mikrofacije krede i starijeg terciara Spoljnih Dinarida Jugoslavije. -
Zavod. Geol. Istraž. Cme Gore. paleont. jugosl. Dinarida (A), 4, 1, 1-35, Titograd.
Radoičič, R. 1969: Aberantna grana fosilnih Tintinina (Podred Tintinnina). La branche
aberrante des Tintinnines fossiles (Sous-Ordre Tintinnina). - Paleont. Jugosl., 9, 5-71, Zagreb.
Savie, D. 1973: Jurassic and Cretaceous beds between Gornje Jelenje and Grobničko polje
(orig. in Croat.). - Geol. vjesnik, 25, 127-147, Zagreb.
Savie, D. & Dozet, S. 1985: Tumač za list Delnice. Osnovna geološka karta SFRJ, 1 :
100 000. - Zvezni geološki zavod, 58 p., Beograd.
Strohmenger, C. & Dozet, S. 1991: Stratigraphy and geochemistry of Jurassic car-
bonate rocks from Suha krajina and Mala gora mountain (Southern Slovenia). - Geologija, 33,
315-331 (1990), Ljubljana.
Šribar, L. 1979 a: Biostratigraphy of Lower Cretaceous beds from the Logatec plain (orig.
in Slov). - Geologija, 22/2, 277-308, Ljubljana.
Šribar, L. 1979 b: Biostratigraphy of the Jurassic-Cretaceous boundary layers from south
Slovenia. - Geologija 22/1, 113-116, Ljubljana.
Šribar, L., G u š i č , I. & Radoičić, R. 1979: Excursion R. (Smrekovec-Vrhnika-Lo-
gatec) - IG"" European micropaleontological colloquium, 247-254, Ljubljana.
Turnšek, D. & Buser, S.1966: The development of the Lower Cretaceous beds and the
boundary between Jurassic and Cretaceous formations in the western part of Trnovski gozd
(orig. in Slov). - Geologija, 9, 527-548, Ljubljana.
Turnšek, D. & Buser, S. 1974: Lower Cretaceous corals, hydrozoans and chaetetids
from Banjška planota and Trnovski gozd (orig. in Slov.). - Razprave SAZU, 4. razr., 81-124, Lju-
bljana.
Turnšek, D., Pleničar, М. & Šribar, L. 1992: Lower Cretaceous fauna from Slo-
venski vrh near Kočevje (south Slovenia) (orig. in Slov.). - Razprave SAZU, 4. razr., 33, 205-257,
Ljubljana.
Uršič, F. 1933: Stratigrafski pregled slojeva u okolini Kočevja u Dravskoj banovini. - Vje-
snik Geol. Inst. Kralj. Jugosl. (1932), 2, 83-106, Beograd.
V	e 1 i ć, I. 1977: Jurassic and Lower Cretaceous Assemblage - zones in Mt. Velika Kapela
(Central Croatia). - Acta Geologica, 42, 9/2, 15-37,Zagreb.
V	e 1 i ć, I. & S o k a č, B. 1978: Biostratigrafska analiza jure i donje krede šire okolice Ogu-
lina (središnja Hrvatska). - Geol. vjesnik 30/1, 309-337, Zagreb.
Plate 1 - Tabla 1
1, 2 Pelmicritic limestone with Chara oogonia (55 x)
Črnomelj, Berriasian-Valanginian
Pelmikritni apnenec z oogoniji haracej Chara sp. (55 x)
Črnomelj, berriasij-valanginij
3	Dismicritic limestone with Chara oogonia (85.5 x)
Kočarji (Kočevska), Berriasian-Valanginian
Dismikritni apnenec z oogoniji haracej Chara sp. (85,5 x)
Kočarji (Kočevska), berriasij-valanginij
4	Biomicritic limestone with Chara oogonia (34 x)
Kočarji (Kočevska), Berriasian-Valanginian
Biomikritni apnenec z oogoniji haracej Chara sp. (34 x)
Kočarji (Kočevska), berriasij-valanginij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 171
172_Stevo Dozet & Ljudmila Šribar
Plate 2 - Tabla 2
1	Biomicritic limestone with fossils Salpingoporella annulata Carozzi and Favreina salevensis
(Paréjas), 34 x
W of Grčarice (Kočevska), Berriasian
Biomikritni apnenec s fosiloma Salpingoporella annulata Carozzi in Favreina salevensis
(Paréjas), 34 x
W od Grčaric (Kočevska), berriasij
2	Biomicritic limestone with fossils Salpingoporella annulata Carozzi and Favreina salevensis
(Paréjas), 13.5 x
Grčarice (Kočevska), Berriasian
Biomikritni apnenec s fosiloma Salpingoporella annulata Carozzi in Favreina salevensis
(Paréjas), 13,5 x
Grčarice (Kočevska), berriasij
3	Pelintrasparitic limestone, Favreina salevensis (Paréjas), 30 x
Mala gora, Valanginian
Pelintrasparitni apnenec Favreina salevensis (Paréjas), 30 x
Mala gora, valanginij
4	Pelmicritic limestone, Favreina salevensis (Paréjas), 30 x
Mala gora, Berriasian
Pelmikritni apnenec Favreina salevensis (Paréjas), 30 x
Mala gora, berriasij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 173
174_Stevo Dozet & Ljudmila Šribar
Plate 3 - Tabla 3
1	Biopelmicrosparitic limestone, Salpingoporella annulata Carozzi (34 x)
W of Grčarice (Kočevska), Barremian
Biopelmikrosparitni apnenec, Salpingoporella annulata Carozzi (34 x)
W od Grčaric (Kočevska), barremij
2	Bioosparitic limestone with microfossils Salpingoporella annulata Carozzi (34 x)
Miliolidae, Ophthalmidiidae, Textulariidae
N of Petekova (Ilirska Bistrica), Valanginian
Biooosparitni apnenec z mikrofosili Salpingoporella annulata Carozzi (34 x)
Miliolidae, Ophthalmidiidae, Textulariidae
N od Petekove (Ilirska Bistrica), valanginij
3	Biomicritic limestone with alga Clypeina ? solkani Conrad & Radoičič (18 x)
South of Korinj, Hauterivian
Biomikritni apnenec z algo Clypeina ? solkani Conrad & Radoičić (18 x)
Južno od Korinj a, hauterivij
4	Dasycladacea limestone, Clypeina ? solkani Conrad & Radoičić (34 x)
SW of Dolenje (Ilirska Bistrica), Hauterivian
Biomikritni apnenec z algo Clypeina ? solkani Conrad & Radoičić (34 x)
SW od Dolenja (Ilirska Bistrica), hauterivij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 175
176_Stevo Dozet & Ljudmila Šribar
Plate 4 - Tabla 4
1	Biopelmicritic limestone, Salpingoporella muehlbergii (Lorenz), 34 x
Črnomelj, Barremian
Biopelmikritni apnenec, Salpingoporella muehlbergii (Lorenz), 34 x
Črnomelj, barremij
2	Biopelsparitic limestone, Salpingoporella muehlbergii (Lorenz), 55 x
Črnomelj, Barremian
Biopelsparitni apnenec, Salpingoporella muehlbergii (Lorenz), 55 x
Črnomelj, barremij
3	Biopelmicritic limestone, Salpingoporella muehlbergii (Lorenz), 43 x
Grelc (Kočevska), Barremian
Biopelmikritni apnenec, Salpingoporella muehlbergii (Lorenz), 43 x
Grelc (Kočevska), barremij
4	Biopelmicritic limestone, Salpingoporella muehlbergii (Lorenz), 55 x
Grelc (Kočevska), Barremian
Biopelmikritni apnenec, Salpingoporella muehlbergii (Lorenz), 55 x
Grelc (Kočevska), barremij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 177
178_Stevo Dozet & Ljudmila Šribar
Plate 5 - Tabla 5
1	Biomicritic limestone, Salpingoporella dinarica Radoičić (24.5 x)
Miliolids, textulariids
Podgozd (Gorica), Aptian
Biomikritni apnenec, Salpingoporella dinarica Radoičić (24,5 x)
miliolide, textularide
Podgozd (Gorica), aptij
2	Biomicritic limestone, Salpingoporella dinarica Radoičić (24.5 x)
Miliolids, textulariids
Stara Cerkev-Vrbovec (Ribnica), Aptian
Biomikritni apnenec, Salpingoporella dinarica Radoičić (24,5 x)
miliolide, textularide
Stara Cerkev-Vrbovec (Ribnica), aptij
3	Brecciated limestone, Salpingoporella dinarica Radoičič (24.5 x)
Miliolids, textulariids
NE of Gomance (Ilirska Bistrica), Aptian
Brečasti apnenec, Salpingoporella dinarica Radoičić (24,5 x)
miliolide, textularide
NE od Gomanc (Ilirska Bistrica), aptij
4	Biopelmicritic limestone, Salpingoporella dinarica Radoičić (18 x)
Konjsko (Kočevje), Aptian
Biopelmikritni apnenec, Salpingoporella dinarica Radoičič (18 x)
Konjsko (Kočevje), aptij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 179
180_Stevo Dozet & Ljudmila Šribar
Plate 6 - Tabla 6
1	Biomicritic Orbitolina limestone, Palorbitolina lenticularis (Blumenbach), 13.5 x
Konjsko (Kočevje), Lower Aptian
Biomikritni orbitolinski apnenec, Palorbitolina lenticularis (Blumenbach), 13,5 x
Konjsko (Kočevje), spodnji aptij
2	Pelmicritic Orbitolina limestone, Palorbitolina lenticularis (Blumenbach), 13.5 x
Suha krajina. Lower Aptian
Pelmikritni orbitolinski apnenec, Palorbitolina lenticularis (Blumenbach), 13,5 x
Suha krajina, spodnji aptij
3	Biomicritic Orbitolina limestone, Orbitolina (Mesorbitolina) ex gr. texana (Roemer), (55 x)
Konjsko (Kočevje), Lower Albian
Biomikritni orbitolinski apnenec, Orbitolina (Mesorbitolina) ex gr texana (Roemer), (55 x)
Konjsko (Kočevje), spodnji albij
4	Biosparitic Orbitolina limestone (18 x)
Logaška planota. Lower Albian
Biosparitni orbitolinski apnenec (18 x)
Logaška planota, spodnji albij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 181
182_Stevo Dozet & Ljudmila Šribar
Plate 7 - Tabla 7
1	Biopelmicritic limestone, Bacinella irregularis Radoičić (30 x)
Mala gora, Aptian
Biopelmikritni apnenec. Bacinella irregularis Radoičić (30 x)
Mala gora, aptij
2	Algal biolitite. Bacinella irregularis Radoičić (30 x)
Fuksov laz (Ribnica), Barremian-Aptian
Algni biolitit. Bacinella irregularis Radoičić (30 x)
Fuksov laz (Ribnica), barremij-aptij
3	Biointramicrosparitic limestone, Pseudotextulariella ? scarsellai (De Castro), 50 x
Črnomelj, Barremian
Biointramikrosparitni apnenec, Pseudotextulariella ? scarsellai (De Castro), 50 x
Črnomelj, barremij
4	Biopelmicrosparitic limestone, Sabaudia minuta (Hofker), 43 x
Konjsko (Kočevje), Aptian
Biopelmikrosparitni apnenec, Sabaudia minuta (Hofker), 43 x
Konjsko (Kočevje), aptij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 183
184_Stevo Dozet & Ljudmila Šribar
Plate 8 - Tabla 8
1	"Valdanchella" dercourti Decrouez & Moullade (65 x)
Logaška planota, Upper Albian
"Valdanchella" dercourti Decrouez & Moullade (65 x)
Logaška planota, zgornji albij
2	Biomicritic limestone, Nummoloculina heimi Bonet (34 x)
Konjsko (Kočevje), Lower Albian
Biomikritni apnenec, Nummoloculina heimi Bonet (34 x)
Konjsko (Kočevje), spodnji albij
3	Biosparitic limestone, Valvulammina picardi Henson (65 x)
Logaška planota. Lower Albian
Biosparitni apnenec, Valvulammina picardi Henson (65 x)
Logaška planota, spodnji albij
4	Biopelmicritic limestone with alga Salpingoporella turgida (Radoičić), 16 x
Črnomelj, Upper Albian
Biopelmikritni apnenec z algo Salpingoporella turgida (Radoičić), 16 x
Črnomelj, zgornji albij
Lower Cretaceous Shallow-Marine Sedimentation and Biota
 185