GEOLOGICA CARPATHICA, JUNE 2008, 59, 3, 211—224
www.geologicacarpathica.sk
The Carnian-Norian basin-platform system of the Martuljek
Mountain Group (Julian Alps, Slovenia): progradation
of the Dachstein carbonate platform
BOGOMIR CELARC and TEA KOLAR-JURKOVŠEK
Geological Survey of Slovenia, Dimičeva ulica 14, SI-1000 Ljubljana, Slovenia; bogomir.celarc@geo-zs.si; tea.kolar@geo-zs.si
(Manuscript received June 14, 2007; accepted in revised form December 13, 2007)
Abstract: In the Martuljek Mountain Group (MMG), positioned in the northern part of the Julian Alps (NW Slovenia),
a widespread drowning of the middle Carnian carbonate platform is marked by the onset of a thin (approximately 25 m)
horizon of reddish pelagic platy basinal limestones (Martuljek platy limestone). According to conodont data, different
ages of the upper part of the Martuljek platy limestone are documented, namely late Carnian in the SW and early Norian
in the NE part of the MMG. The rimmed Dachstein carbonate platform progrades into the basin with typically devel-
oped facies zones: slope and reef margin (approximately 300 m thick) with abundant coral fauna with other framebuilders
and the Lofer cyclic Dachstein Limestone in the backreef peritidal area. In the NW face of the Mt Škrlatica, platform to
the basin transition is spectacularly exposed. The interfingering of slope to basin sediments and the dip of the
clinostratification, indicate SW to NE progradation of the Dachstein platform (in recent orientation), which is also in
accordance with conodont data estimation of the underlying Martuljek platy limestones. The margin of the Dachstein
platform in the MMG is thus progressively younger from the SW direction to the NE. After (and during) the filling of
the basin, the peritidal carbonate platform, with a more than 1 km thick succession of the Dachstein Limestone pre-
vailed until the end of the Triassic Period in the central part of the Julian Alps. The Carnian drowning event in the Julian
Alps and also in the Kamnik—Savinja Alps is not just a locally limited phenomenon, as described so far, but a wide-
spread event, triggering the growth of the Tuvalian—Norian reefs, facing more open marine areas.
Key words: Late Triassic, Slovenia, Julian Alps, carbonate platform progradation, facies analysis, conodonts.
Introduction
According to paleogeographical studies, the Slovenian part of
the Julian Alps formed an isolated platform between the Slove-
nian Basin and the Hallstatt-Meliata Ocean (e.g. Haas et al.
1995; Ziegler & Stampfli 2001; Stampfli & Borel 2002). A
distinct transgression pulse, recognized above the former La-
dinian—Carnian platforms or Raibl Group, deepening, forma-
tion of the basin(s) and progradation of the rimmed Main
Dolomite or Dachstein Limestone platforms, was recognized
in the Julian Alps (Lieberman 1978; Ramovš 1986a,b, 1987;
Jurkovšek 1987a,b; Schlaf et al. 1997a,b; De Zanche et al.
2000; Gianolla et al. 2003). In the Slovenian Basin and in the
western part of the Pokljuka Plateau, basinal sedimentation
persisted through the Norian and Rhaetian (Kolar-Jurkovšek
et al. 1983; Buser 1989; Buser et al. 2007) with coeval reef de-
velopment (Turnšek & Buser 1989). In the nearby Karavanke
Mountains, however, the stratigraphic development of the No-
rian strata differs strongly. In the Košuta Unit, Dachstein
Limestone is developed in the Norian (Kolar-Jurkovšek et al.
2005), while basinal sedimentation persisted through the Lias-
sic in the Hahnkogel area (Krystyn et al. 1994; Schlaf 1996).
The Tuvalian deepening event and stratigraphically very simi-
lar developments are also recognized in the Kamnik—Savinja
Alps around 50 km to the east (Ramovš 1989; Jamnik & Ra-
movš 1993).
The progradation geometry of the Upper Triassic Carnian—
Norian carbonate platform in the Julian Alps (Slovenia) is of-
ten difficult to study because of the strong Alpine tectonics
and hence rarely preserved stratigraphic successions (in the di-
rection of the platform progradation, that is perpendicular to
the clinostratification). Transitions from basinal to platform
sediments often coincide with important detachment horizons.
An excellent seismic scale section was described by Gianolla
et al. (2003) in the Portella (near Cave del Predil) close to the
Italian-Slovenian border with the progradation of the Main
Dolomite platform in the SSW—NNE direction. In the Martul-
jek Mountain Group (MMG), another tectonically relatively
undisturbed basin to platform transition (also considerably lat-
erally extended) is discussed in this paper.
Before the pioneering study of Ramovš (1986a), little was
known about the upper Carnian—lower Norian basinal sedi-
ments in the northern part of the Julian Alps. The Tuvalian pe-
lagic, red, platy, ammonoid rich limestones of the Hallstatt
facies were described in the Mt Razor and Mt Planja area, as
part of the Kriški podi Plateau, SW of the MMG (Ramovš
1987; Sattler 1998) and on top of the Mt Kukova špica (Ra-
movš 1986a) in the NE part of the MMG. These studies were
spatially confined, and the extension of the basinal sediments
between the aforementioned areas (the central part of the
MMG) was unknown until recently (Celarc 2006; Celarc &
Ogorelec 2006). The Norian-Rhaetian reef limestones are
much better studied (Turnšek & Ramovš 1987; Ramovš &
Turnšek 1991).
The main goal of the present paper is to describe the archi-
tecture of the facies belts of the prograding platform, based on
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CELARC and KOLAR-JURKOVŠEK
the detailed mapping and conodont analysis of the basinal
platy limestones. We introduced a new (informal) name for
this lithological unit as the Martuljek platy limestone. Besides
determining the direction of progradation, we estimated sedi-
mentation rates (filling of the basin) and the dynamics of the
platform’s growth.
Geological background and location
The study area belongs to the Julian Alps (NW Slovenia)
(Fig. 1), which along with the eastern lying Kamnik—Savinja
Alps, forms the so-called Julian Nappe. Along with the south-
erly positioned Tolmin Nappe it represents the easternmost
continuation of the Southern Alps (Placer 1999; Haas et al.
2000) extended from NE Italy. On their north side part the
Julian Alps are separated from the South Karavanke Moun-
tains by the dextral strike slip Sava fault. Paleogeographically,
the Julian Nappe in the Upper Triassic belonged to the rela-
tively uniform Julian Carbonate Platform, bound to the south
with the deeper Slovenian Basin (Buser 1989). In the Norian,
the Julian Alps were located on the passive margin of the
southern shelf of the Hallstatt-Meliata branch of the Neo-
Tethys (Haas et al. 1995; Ziegler & Stampfli 2001). During
the Late Triassic, a different paleogeographical environments
were formed. In the western (Italian part), the terrigenous in-
fluenced Raibl Group filled previous basins in the Julian and
early Tuvalian (Gianolla et al. 2003; Preto et al. 2005). In the
eastern (Slovenian) part of the Julian Alps, reefs and platform
sedimentation persisted continuously from the late Ladinian to
the beginning of the Tuvalian periods (Ramovš & Turnšek
1984; Jurkovšek 1987b).
The MMG is geographically positioned in the Northern
Julian Alps, bordered to the north by the Upper Sava Valley,
to the east by the Vrata Valley, to the south by the Kriški
podi Plateau and to the west by the Pišnica and Krnica Val-
leys. The researched area is bounded by the north vergent
Tamar backthrust, and NE—SW directed strike-slip faults in
the west and east, respectively. The studied area thus belongs
to a relatively subsided tectonic block, internally slightly de-
formed, with strata generally dipping gently to the south
(Fig. 2).
Stratigraphy
Since there are no officially accepted names for formations,
we use informal names taken from various works of previous
Fig. 1. Location (rectangle) of the research area (Martuljek Mountain Group, Julian Alps, Slovenia). Tectonic units after Placer (1999).
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CARNIAN-NORIAN BASIN-PLATFORM SYSTEM (JULIAN ALPS): CARBONATE PLATFORM PROGRADATION
authors. The geological succession is composed from bottom
to top as (Fig. 3):
1) Razor limestone (lower Carnian) as proposed by Ramovš
(1987), consisting of cyclic bedded limestones and massive
reef limestones;
2) Martuljek platy limestone (upper Tuvalian – Ramovš
(1986a); upper Tuvalian—lower Norian in this paper), consist-
ing of reddish, platy pelagic limestones;
3) Dachstein reef limestone (upper Tuvalian—lower Norian),
consisting of hard-to-distinguish slope and reef margin facies;
4) Dachstein Limestone (Norian—Rhaetian), consisting of
cyclic bedded limestones (Jurkovšek 1987a,b).
Razor limestone (lower Carnian)
Ramovš (1987) described a new calcareous formation and
named it Razor (after Mt Razor) limestone, forming a footwall
below the thin horizon of the Hallstatt type Tuvalian platy
limestone (Martuljek platy limestone in this article). He distin-
guished between two lithologic types of Razor limestone:
– Thick-bedded grey to brownish micritic limestone with
transition to trombolitic, oncoidic and pseudooncoidic lime-
stones (bedded peritidal Razor limestone);
– Biolithic reef limestone, with small patch reefs. Coral-
lites are overgrown with spongiostromata crusts. Margaros-
milia sp. is abundant, together with sponge Ceotinella
mirunae and Uvanella sp. There are many patch reefs with
corals of Retiophyllia type and bioclastic reef detritus between
mounds (Razor reef limestone).
The age of the limestones is not entirely clear. According to
Ramovš (1987) the reef limestone is similar to the Carnian Ti-
sovec Limestone from the Western Carpathians (Kollarova-
Andrusova 1960) and is probably early Carnian.
In the MMG only bedded peritidal Razor limestone is
present. The maximum thickness is around 400 m (Mt Široka
peč). Under Mt Mali Oltar and Mt Velika Ponca it reaches
around 100—200 m and passes downwards into massive dolo-
mites. The bedded Razor limestone is in tectonic contact with
Middle Triassic limestones west of Mt Škrlatica, Mt Rakova
špica and Mt Rogljica.
The bedded peritidal Razor limestone is organized into 1—
1.5 m thick, predominantly shallowing upward asymmetric
cycles (Fig. 4.1).
Subtidal deposits are characterized by thick-bedded pack-
stone and grainstone with variable amounts of pellets, peloids,
oncoids and intraclasts. Skeletal grains are composed of green
algae and foraminifers. Shallower subtidal facies are repre-
sented by abundant oncoidal horizons with a maximum thick-
ness of 20 cm (Fig. 4.2). The origin of oncoids is probably
associated with a slightly more agitated environment, with tid-
al channels in which tidal currents enabled constant move-
ment and their concentric growth.
Intertidal-supratidal facies are recognizable by laminated
grainstones, which are often dolomitized, and with horizontal
microbial laminites. Fenestral pores (loferites) are very com-
mon in these horizons. They are often developed as microbial
boundstones, forming typical bedding parallel cracks and
birdseye pores (Fig. 4.3) Desiccation structures could also be
found in the wackestone—packstone facies (Fig. 4.4) and in the
upper parts of the oncoidal horizons (Fig. 4.5). Tepee stuc-
tures are also abundant, represented as low relief antiforms
(Fig. 4.6). Cavities of the tepee walls are filled with laminated,
Fig. 2. Geological sketch map of the Martuljek Mountain Group. For location see Fig. 1.
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CELARC and KOLAR-JURKOVŠEK
often reddish calcite crusts. Flat lying rip up clasts up to 20 cm
long and 5 cm thick occur in distinct horizons. They are inter-
preted as tempestites. The groundmass consists of the carbon-
ate matrix.
Exposure surfaces are found at the top of some (rare) sub-
tidal and intertidal—supratidal deposits. These intervals are
usually very thin (up to 10 cm) with an uneven disconformi-
ty surface, overlain with matrix supported breccia with clasts
eroded from underlying shallow-subtidal and intertidal su-
pratidal limestones. These breccias suggest a short lived in-
terruption in deposition. The matrix is usually yellow silt
and residual carbonate clay. Angular to subangular black
pebbles are common constituents in the breccia horizons and
they are also scattered in the lower part of the subsequent
subtidal horizon.
Fig. 3. Schematic late Julian—early Norian stratigraphy in the Mar-
tuljek Mountain Group.
Martuljek platy limestone (upper Tuvalian—lower Norian)
The reddish, platy, pelagic upper Tuvalian limestones were
described by Ramovš (1986a, 1987) in the areas of Mt Razor,
Mt Planja (Kriški podi Plateau), Mt Kukova špica (MMG),
Kozja Dnina, Mlinarica and Macesnovec (Mt Triglav area).
Tuvalian platy limestones from the latter three locations are
shown in the Basic Geological Map of Slovenia (Jurkovšek
1987a), and biostratigraphic study of these strata documented
the conodont faunas of the polygnathiformis and nodosa
Zones (Jurkovšek et al. 1984; Kolar-Jurkovšek 1991). Based
on findings of the ammonites Projuvavites jaworskii, Dis-
cotropites plinii, and conodonts Epigondolella nodosa and
Neogondolella polygnathiformis on Mt Razor, Ramovš
(1986a) assigned this horizon to the upper Tuvalian, Anatro-
pites Zone – the plinii subzone, and according to their litho-
logical similarity compared these limestones to the Hallstatt
Limestones of the Northern Calcareous Alps.
In the MMG, except on Mt Kukova špica, the red pelagic
platy limestones of the Hallstatt type were mapped and de-
scribed for the first time. On the summit of Mt Kukova špica
only their lower part is preserved as an erosional remnant. On
the basis of conodonts and ammonites, Ramovš (1986a) as-
signed the limestones from Mt Kukova špica to the upper Tu-
valian, Anatropites Zone.
As this horizon does not have any formation name, we refer
to it as the Martuljek platy limestone. The Martuljek platy
limestone extends from the northeastern face of Mt Rogljica,
Mt Rakova špica and Mt Škrlatica, the northeastern and east-
ern faces of Mt Velika Ponca and the northern face of Mt Mali
Oltar, Mt Široka peč and Mt Škrnatnarica (Fig. 2). From the
top of Mt Kukova špica, it continues in a southern direction
towards the Vrata Valley. The strata dip predominantly in a
southern direction with a moderate inclination of 10—20° and
attain a maximum thickness of 25 m.
Two members are distinguished in the Martuljek platy lime-
stone (Fig. 5).
The Lower Member is composed of reddish (rarely grey-
ish) sometimes indistinctly bedded (Fig. 4.7), pelagic lime-
stone (bioclastic wackestone to packstone). It is organized in
10—20 cm thick beds with wavy to planar bedding. Thin (up to
5 mm) intercalations of reddish to green silt frequently occur
on the bedding planes and are also randomly scattered in the
beds. Stilolitic seams parallel to the bedding planes are often
developed, indicating chemical compaction. Some beds in the
lower part of succession are rich in ammonoids, gastropods
and brachiopods. Green glauconite grains are also present in
some samples, testifying to the slow rate of the sedimentation.
The main facies type is bio-intra clastic packstone rich in fora-
minifers, brachiopod shells, calcified spicula, pellets, crinoids,
ostracodes (Fig. 6.1) and is often dolomitized (Fig. 6.2). The
Lower Member overlies sharply, without paleorelief, peritidal
bedded Razor limestone (Fig. 6.3), that is occasionally also
reddish around the contact and sometimes some meters below.
The succession of pelagic Martuljek platy limestone on the
shallow water Razor limestone represents a major drowning
unconformity and is identical to the Mt Razor area (Sattler
1998). The reason for the drowning is not entirely clear, but
this event is widespread over a broad area (Lieberman 1978;
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CARNIAN-NORIAN BASIN-PLATFORM SYSTEM (JULIAN ALPS): CARBONATE PLATFORM PROGRADATION
Krystyn et al. 1994; Schlaf 1996; De Zanche et al. 2000; Gi-
anolla et al. 2003). It is probably connected with rapid relative
sea-level rise caused by strong extensional tectonic pulse at
the beginning of the 3
rd
-order, No. 1 depositional sequence in
the Southern Alps, which also corresponds to the lower
boundary of a 2
nd
-order cycle (Gianolla et al. 1998). A similar
situation is reported from the Northern Calcareous Alps
(Mandl 2000).
Fig. 4. Facies of the Razor limestone (1—6) and Martuljek platy limestone, Lover Member (7). 1 – Bedded peritidal Razor limestone. Cy-
clic alternation of subtidal and intertidal oncoidal—loferitic limestone. Kačji jezik (KJ) section, scale bar 1 m. 2 – Oncoid horizon, Kačji
jezik (KJ) section, scale bar 4 cm. 3 – Microbial boundstone with loferitic shrinkage cracks and some birds eyes pores, filled with stalac-
tite and blocky cement. Skrlatica (ŠK) section, sample ŠK20, scale bar 2 mm. 4 – Wackestone—packstone with loferitic pores. Kačji jezik
(KJ) section, sample KJ16, scale bar 2 mm. 5 – Pisoid rudstone—oncoid grainstone with shrinkage pores. Pisoid—oncoid nuclei consist of
pellets and intraclasts. Kačji jezik (KJ) section, sample KJ16, scale bar 2 mm. 6 – Tepee in the laminated loferitic limestone. Kačji jezik
(KJ) section, scale bar 10 cm. 7 – Indistinctly bedded red micritic Martuljek platy limestone, Lower Member, Kačji jezik (KJ) section,
hammer (32 cm long) for the scale.
The Upper Member is composed of light grey to white
platy and thin-bedded, often dolomitized limestones (coral
and crinoid grainstones and rudstones), showing a tendency
towards upward bed thickening (in the lower part 20 cm, in
the upper part 45 cm). The bedding is more clearly pro-
nounced than in the Lower Member. In the detritic limestone
(rudstone), normal gradation is evident, expressed with the
reef detritus in the horizons with a sharp planar or irregular
216
CELARC and KOLAR-JURKOVŠEK
erosional lower boundary and gradual upper boundary with
overlying grainstone (Fig. 6.4). Reef debris is frequently dolo-
mitized and the primary structure is strongly obliterated
(Fig. 6.5). Beds of the red pelagic limestone are often found
between reef detritus, indicating a temporary break in the
shedding of material from the platform. As the Upper Member
passes upward into the slope limestones, we interpret these de-
posits as the toe of the slope facies. Graded grainstones and
rudstones near the toe of the slope are redeposited shallow wa-
ter sediments (reef margin with abundant corals, sponge and
other biota) during sea-level highstands in the form of turbidit-
ic flows. Similar graded grainstones are reported from the La-
dinian Latemar buildup in the Dolomites (Goldhammer &
Harris 1989). Slight lateral thinning of individual strata in a
seaward direction, namely in the direction of the progradation
of the platform, can be noted in some places.
The Martuljek platy limestone shows a shallowing upwards
trend with an increasing amount of platform derived clasts
(reef debris, algal remnants) and abundant stems and plates of
crinoids from the slope environment.
Conodont fauna from the Martuljek platy limestone
Seven conodont samples were collected from three sections
(B1, JG and ŠP) (Table 1, Fig. 2, Fig. 5), where the Martuljek
platy limestone is exposed, between Razor limestone in the
footwall and the slope of the Dachstein reef limestone in the
hangingwall. Their WGS 84 coordinates in fractional degrees
and elevations are: B1: lat = 46.438509, lon = 13.819957,
elevation = 2140 m;
JG: lat = 46.441170,
lon = 13.83905,
elevation = 2220 m;
ŠP: lat = 46.44134,
lon = 13.83993,
elevation = 2220 m.
Sections were chosen according to positions relative to the
direction of the Dachstein platform progradation in order to
test the age of the uppermost part of the Martuljek platy lime-
stone. Due to difficult access and very steep mountain terrain,
composite (and not bed-by-bed) test sampling was carried out
in order to document conodont fauna in the investigated sec-
tion and in order to ascertain the potential for future establish-
ment of conodont biozonation intervals. Therefore, only an
estimated age assessment can be made based on the obtained
results. For detailed paleontological study that would enable
the introduction of precise conodont biozonation, bed-by-bed
sampling would be required. For this study we collected com-
posite samples, with most three samples and at least one sam-
ple per section, with a weight of 1—1.5 kg.
Conodonts are white with CAI = 1 (Epstein et al. 1977) indi-
cating an average thermal overprint of 65 °C.
The determined conodont taxa are shown in Table 1. Am-
monoid and conodont biostratigraphic zonations for the upper
Carnian and lower Norian (Gradstein et al. 2004) are shown in
Table 2.
Faunas are marked by the Carnepigondolella, Epigondolel-
la and Metapolygnathus species (Fig. 7). In this report a taxo-
nomic differentiation of Orchard (1991a) and Kozur (2003) is
adopted: Metapolygnathus ranges throughout the Carnian and
into the basal Norian, but Epigondolella is restricted only to
the Norian, while the recently established Carnepigondolella
is a marker of the upper Carnian.
Metapolygnathus is characterized by reduced platforms that
may have ornamented (nodes) platform margins. A basal pit is
usually situated in the posterior part of the platform. On the
contrary, the genus Epigondolella has a more reduced plat-
form with lateral platform denticles of considerable height. A
well marked free blade is developed. A basal pit is usually sit-
uated beneath the centre of the platform (Orchard 1991a).
Carnepigondolella is regarded as the forerunner of Epigon-
Fig. 5. Stratigraphical column of the Martuljek platy limestone (Mt
Škrlatica (ŠK) section), and results of conodont analysis from other
sections (see text and Fig. 2 for the location).
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CARNIAN-NORIAN BASIN-PLATFORM SYSTEM (JULIAN ALPS): CARBONATE PLATFORM PROGRADATION
Fig. 6. Facies of the Martuljek platy limestone, Lower Member (1—3), Upper Member (4, 5). 1 – Bio-intra clastic packstone. Škrlatica
(ŠK) section, sample ŠK19, scale bar 1 mm. 2 – Bio-intra clastic slightly dolomitized packstone, Škrlatica (ŠK) section, sample ŠK20,
scale bar 2 mm. 3 – Contact between Razor limestone (lower part of the photo) and Martuljek platy limestone (upper part of the photo) is
sharp and shows no relief. Jugova grapa (JG) section, marker pencil (8 cm long) for the scale. 4 – Graded reef debris with sharp lower
boundary. Jugova grapa (JG) section, scale bar 4 cm. 5 – Strongly dolomitized reef debris with crinoid plates. Jugova grapa (JG) section,
sample JG2, scale bar 2 mm.
dolella and is characterized by the presence of nodes or broad
and short denticles on the platform margins and by a subtermi-
nal basal pit (Kozur 2003).
In the studied material ornate gondolellid forms predomi-
nate, but the presence of unornamented forms (M. communisti,
M. polygnathiformis) have been recorded in two samples only.
The conodont faunas of the collected samples markedly
characterize the Carnian-Norian boundary interval. During the
last period of investigations in many countries, several sug-
gestions to define the Carnian—Norian boundary (CNB) have
been made (Orchard et al. 2000; Krystyn & Gallet 2002). In
some older proposals the FAD of Norigondolella navicula
have been utilized to mark the base of the Norian (Krystyn
1980; Orchard 1991a). Yet the species is ecologically con-
trolled and thus its entry is not reliable for comparison (Or-
chard et al. 2000; Krystyn & Gallet 2002; Kozur 2003).
Upper Triassic conodont zonation has been considerably re-
fined based on data from British Columbia (Orchard 1991b).
Well documented faunas of the CNB interval have just recent-
ly been demonstrated by Orchard (2007). In a short succession
at Black Bear Ridge in British Columbia, spanning the Wel-
leri 2 through Kerri ammonoid zones, seven conodont datums
defining eight faunal intervals can be identified. They are
based on a detailed study of progressive evolutionary changes
that enable recognition of several morphogenetic lineages (Or-
chard 2007).
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CELARC and KOLAR-JURKOVŠEK
A recent suggestion to define the CNB based on the FAD of
Epigondolella quadrata has been put forward among con-
odont workers and members of the Subcommission on Trias-
sic Stratigraphy (personal communication). It should be
mentioned that in Kozur’s (2003) integrated ammonoid, con-
odont and radiolarian zonation of the Triassic Epigondolella
quadrata Zone is equivalent to the upper Kerri and lower
Paulckei ( = Dawsoni) zones. As this proposal has not been
formally accepted by international geological institutions, this
datum can currently be considered only as a potential candi-
date.
On the basis of the composition of the examined faunules
and taking into account above mentioned data, the following
conclusions can be made:
1) samples BI-1 and JG-1 are marked by M. polygnathifor-
mis. This element is accompanied by Metapolygnathus n. sp. G
Orchard (forerunner of M. primitius) or M. carpathica and
Carnepigondolella samueli. The absence of epigondolellids is
evident. Age: late Carnian.
2) samples ŠP-1, ŠP-2 and JG-2 are mixed late Carnian—ear-
ly Norian in age due to the co-occurrence of Carnepigondolel-
la, Epigondolella and Metapolygnathus forms.
3) sample ŠP-3 is characterized by the exclusive presence of
Epigondolella species, including E. quadrata. Age: early No-
rian.
Dachstein reef limestone (upper Tuvalian—lower Norian)
Dachstein reef limestones in the MMG are represented with
obviously a very narrow reef crest (margin) and up to 300 m
thick slope toward the basin (fore-reef area) as evident from
the natural cross-sections of the MMG. Because it is macro-
scopically almost impossible to distinguish between the reef
margin, positioned immediately below the bedded Dachstein
Limestone, and the slope, we named the entire lithological
unit of predominantly massive unbedded limestones as the
Dachstein reef limestone. Corals are the most important and
prevailing reef builders; sponges and hydrozoans are subordi-
nate (Turnšek & Ramovš 1987).
On Mt Planja and Mt Razor (Ramovš & Turnšek 1991) the
Dachstein reef limestone complex is up to 150 m thick, but the
actual thickness is unknown because the upper parts are erod-
ed. Coral genera present in the Dachstein reef limestone are
Cyclophyllia, Pokljukosmilia, Protoheterastraea and Rhopa-
lodendron. Three of them are also known from the Tuvalian of
the Pokljuka Plateau (Turnšek & Buser 1989). According to
Sattler (1998), the reef complex on Mt Razor is upper Tuval-
ian, based on the upper Carnian pelagic micrite filling of the
fissures in the Dachstein reef limestone. On Mt Dovški križ,
Mt Šplevta and Mt Kopica, the reef complex is up to 1000 m
thick (Turnšek & Ramovš 1987). The main framebuilders in
the MMG are corals and subordinately sponges, which are
also significant for the Norian—Rhaetian reefs in other areas
(Riedel 1991; Flügel & Senowbari-Daryan 1996; Turnšek
1997). The most abundant corals are the branching forms
Gillastraea, Retiophyllia, Elysastraea and Parathecosmilia
and massive Astraeomorpha and Toechastraea. According to
the geological mapping and observations in the NW face of
Mt Škrlatica, the thickness of the reef complex between the
underlying basinal Martuljek platy limestone and the overly-
Table 1: Conodont taxa determined from sections B1, JG and ŠP. For the geographical position of the sections see Fig. 2, for composite
sample position in lithological column see Fig. 5. Selected conodont taxa are shown in Fig. 7.
Table 2: Ammonoid and conodont biostratigraphic zonations for
the upper Carnian and lower Norian (Gradstein et al. 2004).
219
CARNIAN-NORIAN BASIN-PLATFORM SYSTEM (JULIAN ALPS): CARBONATE PLATFORM PROGRADATION
ing bedded Dachstein Limestone of the interior platform is
around 300 m. This is opposed to finding of Ramovš (1986a,
Fig. 2) and Turnšek & Ramovš (1987) for the Dovški križ
area, where it is estimated to be greater than 1000 m. In our
opinion, this is just an apparent thickness, because dipping of
the strata is directed along the mountain slopes and the reef
occupies a relatively extensive area (Fig. 2). Perhaps the most
prominent mountain built of Dachstein reef limestone in the
MMG is Mt Mali Oltar (Fig. 8.1). During our fieldwork, we
also collected some samples with corals from the top of Mt
Velika Ponca. D. Turnšek determined the Norian species Re-
tiophyllia norica (Fig. 8.2). Coarse-grained breccia or boul-
ders derived from the top of the platform are completely
missing at the toe of the slope and only rudstone with re-
Fig. 7. Conodonts from the Martuljek platy limestone. 1—3 – Mixed upper Carnian-lower Norian faunas. 1a—c – Metapolygnathus commu-
nisti (Hayashi), sample ŠP-1 (GeoZS 4067). 2a—c – Metapolygnathus n. sp. G (Orchard), sample JG-1 (GeoZS 4070). 3a—c – Epigondolella
quadrata (Orchard), sample JG-2 (GeoZS 4071). 4—6 – Upper Carnian, sample BI-1 (GeoZS 4065). 4a—c – Carnepigondolla samueli (Or-
chard). 5a—c – Metapolygnathus polygnathiformis (Budurov & Stefanov). 6a—c – Metapolygnathus carpathicus (Mock). 7—9 – Lower Nori-
an: sample ŠP-3 (GeoZS 4069). 7a—c – Epigondolella quadrata (Orchard). 8a—c – Epigondolella aff. spatulata (Hayashi). 9a—c –
Epigondolella triangularis (Budurov). Scale bar = 100
µm.
worked reef particles and plates of crinoids is present
(Fig. 8.3,4).
Piller (1981) explains the absence of breccias as the result of
water agitation generally being too weak to produce large
boulders from the reef framework.
Dachstein Limestone (?upper Tuvalian, Norian, Rhaetian)
Peritidal bedded Dachstein Limestone rests with a sharp
boundary above the massive Dachstein reef limestone and was
deposited on the broad area behind the prograding reef rim. It
extends between Mt Visoki Rokav on the north and Mt Stenar
in the south (Fig. 2), where it is overlain by Jurassic oolitic
limestone and attains a thickness of around 1000 m with char-
220
CELARC and KOLAR-JURKOVŠEK
acteristic cyclic Lofer (sensu Fisher 1964) development. Sub-
tidal member C consists of 1—3 m thick beds, predominately
wackestone and packstone, subordinately bioclastic rudstone.
Megalodontids and gastropods are abundant in distinct hori-
zons. Solution carstic vugs, filled with reddish silt or isopac-
hous cement, are often present in the upper part of the subtidal
unit, indicating sudden emersions and subsequent carstifica-
tion. Black pebbles are common. Often basal member A is not
developed and laminated fenestral limestone of intertidal
member B directly overlies subtidal unit C (cf. Enos & Sa-
mankassou 1998). Fenestrae are filled with white cement. In
the eastern part of the Julian Alps Dachstein Limestone ex-
tends through the entire Norian and Rhaetian stages, while
further west, the lower part consists of Main Dolomite (Jurk-
ovšek 1987a; Cozzi & Hardie 2003; Gianolla et al. 2003;
Cozzi et al. 2005).
Progradation of the Dachstein platform
The progradation geometry of the Dachstein platform pass-
ing into the basin is exposed in the northwest face of Mt Škrla-
tica parallel to the direction of the platform advance
(Fig. 9a—c). Interfingering of thin-bedded reef-debris lime-
stones (Martuljek platy limestone – Upper Member) and cli-
nostratificated reef-debris limestones of the slope facies
(Dachstein reef limestone) is clearly visible. The lithological
boundary in Mt Škrlatica can be interpreted as a climbing pro-
gradadion in the sense of Bosellini (1984), yet generally, the
boundary is horizontal. The thin-bedded limestones exhibit
low angle onlap against the upper boundary of the intermedi-
ary wedge of the slope limestone intercalated in the Martuljek
platy limestone (Fig. 9c, detail). The Upper Member of the
Martuljek platy limestone slightly thickens basinward, while
individual beds thin in the same direction.
We consider interfingering to be just a local phenomenon.
Namely, elsewhere, it is not expressed and its boundary is
sharp, although clinoforms are still visible. Clinoforms are ex-
pressed as discontinuities in the slope limestones with an in-
clination of around 15—25° and dip in the NE direction
(Fig. 9b,c). Their configuration is oblique-parallel. We as-
sume that underlying Martuljek platy limestone and overlying
Dachstein Limestone were deposited horizontally and their
tectonic dip in the northwest face of Mt Škrlatica is now
slightly (5—10°) to the SSW. If we remove the later tectonic
dip, the true depositional dip of the clinoforms shows only mi-
nor change. In other localities, the contact between the slope
limestones and thin-bedded reef debris is sharp and shows no
interfingering. The clinoform surfaces seem to be absent or are
poorly exposed. We interpret this pattern as the horizontal
downlap plane (Bosellini & Stefani 1991; Maurer 2000)
which indicates rapid progradation of the platform.
The upper boundary of the slope and the margin with the
Dachstein Limestone is almost horizontal in Mt Oltar (toplap
Fig. 8. Facies of the Dachstein reef limestone. 1 – Mt Mali Oltar is built of autochthonous Dachstein reef limestone and allochthonous reef
debris (slope) limestones (height of the face app. 200 m). For location, see Fig. 2. 2 – Coral Retiophyllia norica (det. D. Turnšek). Reef
crest of the Mt Velika Ponca. For location, see Fig. 2. 3 – Coral-crinoid rudstone, slope facies, Kačji jezik (KJ) section, sample KJ5, scale
bar 2 mm. 4 – Coral-crinoid rudstone, Škrlatica (ŠK) section, sample ŠK14, scale bar 2 mm.
221
CARNIAN-NORIAN BASIN-PLATFORM SYSTEM (JULIAN ALPS): CARBONATE PLATFORM PROGRADATION
Fig. 9. Facies interpretation and progradational geometry in the NW face of Mt Škrlatica (Martuljek Mountain Group). a – Small scale fa-
cies interpretation. Arrows indicate contact between Dachstein reef limestone (slope and margin facies) and bedded Dachstein Limestone
(inner platform facies). For location see also Fig. 2. b – Photo of area indicated by rectangle in a. c – Interpretation of facies relationship
with detail of toe of slope interfingering between Martuljek platy limestone (Upper Member) and Dachstein reef limestone. For detail ex-
planation see text.
222
CELARC and KOLAR-JURKOVŠEK
sensu Bosellini 1984) and perhaps a slightly low angle lap off
against a massive margin is visible in Mt Škrlatica (Fig. 9a, ar-
rows indicate contact between massive Dachstein reef lime-
stone and bedded Dachstein Limestone). This relationship
points to the stillstand in the sea level during the early Norian
and progradational dominated highstand systems tract (Wright
& Burchette 1996).
The coral reef margin in the upper part is macroscopically
similar to the slope, so its exact thickness is unknown. Based
on the clinoform dip, the progradation is in the SW—NE direc-
tion, analogous to the trend of the upper Tuvalian Dolomia
Principale in the Portella section (Italy), 16 km to the W (Gia-
nolla et al. 2003). The basinal limestones are also progressive-
ly younger in this direction. According to the Triassic
sequence stratigraphy patterns of the Southern Alps, they rep-
resent the beginning of the No. 1 depositional sequence (Gia-
nolla et al. 1998).
Discussion
The Carnian—Norian lithostratigraphic developments exhib-
it a distinctive heterogeneity in the scale of the Julian Alps.
During the late Julian time, in the Cave del Predil area, the
pre-existing interplatform basin was completely filled, while
the rimmed carbonate platforms (Cassian Dolomite) with
framebuilding organisms underwent strong crisis and were re-
placed by a carbonate-terrigenous ramp (Gianolla et al. 2003;
Preto et al. 2005). However, in the MMG shallow platform
sedimentation persisted through the early Carnian, when the
bedded peritidal and reef Razor limestones were deposited.
Terrigenous “Raibl” beds are not present in this area and the
same is true for the Kamnik—Savinja Alps (Ramovš 1989). In
the Slovenian Basin, positioned further east, basinal Carnian
Amphiclina beds and Norian—Rhaetian cherty Bača Dolomite
were deposited (Buser 1989). During the Tuvalian, strong sub-
sidence affected the area of the Julian Carbonate Platform,
with sedimentation of the basinal Carnitza Formation in the
Cave del Predil area (Lieberman 1978; De Zanche et al. 2000;
Gianolla et al. 2003). In the Vrata Valley, east of the MMG,
Tuvalian and also Lacian basinal limestones are present (Ram-
ovš 1986a; Schlaf et al. 1997a,b). Schlaf et al. (1999) described
thick coquina accumulations in the lower Norian carbonate
slope of the Vrata Valley. The corals are very rare and the mar-
gin of Dolomia Principale in the Cave del Predil is serpulid and
microbial dominated (Gianolla et al. 2003). On the other hand,
corals are abundant in the rim of the synchronous or slightly
younger prograding Dachstein platform in the MMG.
On the basis of conodont age-dating, some rough estima-
tions of the growth mode of the Dachstein platform in the
MMG can be made. The platform prograded in the SW-NE di-
rection as shown by the dip of clinoforms in the NW face of
Mt Škrlatica. The lateral extent of the basinal Martuljek platy
limestones from Mt Razor in the SW, to the Mt Široka peč in
the NE is around 5 km which is also the total (visible) progra-
dation. Conodonts of the late Tuvalian age (Macrolobatus
Zone) were reported for the Mt Razor area (Ramovš 1986a),
but our recent study revealed early Norian age (Kerri—Dawso-
ni Zone) for the upper part of the Mt Široka peč section (this
paper). According to the ICS timescale (Gradstein et al. 2004),
the Macrolobatus and Kerri Chron has a duration of about
3.4 Myr and the Dawsoni Chron about 1.8 Myr. The platform
prograded at least through the entire Macrolobatus Chron, the
whole Kerri Chron, and at least until the middle part of the
Dawsoni Chron (Table 2), that is about 4.3 Myr in total. The
progradation rate is thus estimated at 1200 m/Myr. Nothing
can be said about the aggradation rate of the Dachstein Lime-
stone because of its unfavourable position on the reef margin
(it is mainly eroded). In Cave del Predil, the Tuvalian progra-
dation of the Main Dolomite platform is estimated at 4600 m/
Myr (Gianolla et al. 2003), based on Gradstein et al. (1994),
but this was corrected to around 2700 m/Myr based on new
durations of the ammonite zones (Gradstein et al. 2004). This
approximates to the Ladinian platforms in the Dolomites. In
fact, for better estimation of the rate of platform progradation,
a detailed bed-by-bed resampling should be performed. Se-
quence stratigraphy and paleogeography supported by con-
odont age-dating of the MMG shows some interesting
comparisons between the neighbouring areas, particularly
with stratigraphic successions in the Vrata Valley.
In the MMG, the Lower Member of the Martuljek platy
limestone (Tuvalian) represents the TST (transgressive sys-
tems tract), while the Upper Member, the Dachstein reef lime-
stone and the Dachstein Limestone belong to the HST
(highstand systems tract). In the Vrata Valley in a relatively
limited area, Schlaf et al. (1997a) recognized another HST and
TST around the Carnian-Norian boundary, positioned be-
tween the TST and HST of the MMG. This points to the tec-
tonic control of systems tracts within a broader area.
Sedimentary succession in the Vrata Valley consists of 80 m
thick cherty, bituminous wacke- and mudstones of Tuvalian
age (TST) (Kolar-Jurkovšek 1991), followed by 150 m thick
lower Norian bedded allodapic limestones (HST), that are
overlain by 15—20 m thick bituminous mud- and wackestones
(TST) and 500 m thick lower Norian clinoforms of rapidly
prograding platform and capped with Dachstein Limestone
(HST) (Jurkovšek 1987a).
In the Vrata Valley, an obviously accelerated subsidence
along synsedimentary faults (?halfgraben) came into being
during the late Tuvalian pelagic episode, manifested with
greater thickness and different facies of basinal sediments
when compared with the MMG. The Dachstein platform be-
gun to prograde from the SW and filled the relatively elevated
basinal areas of the MMG (condensed sedimentation). How-
ever, it was not able to completely fill the relatively subsiding
area in the Vrata Valley, which led to the development of the
small restricted intraplatform basin engraved in the Dachstein
platform behind the main prograding rim that is positioned
further towards the NE. Finally, the basin was filled with NE—
SW prograding bivalve dominating clinoforms, and ultimately
the entire area was blanketed by a thick succession of the
Dachstein Limestone. The MMG facies architecture is similar
to some facies reconstructions in the Northern Calcareous
Alps (Mandl 2000), particularly to the Tonion and Hohe
Wand facies, where the Dachstein platform progrades over the
drowned part of the Wetterstein Platform in the direction of
the deep shelf of the Meliata realm.
223
CARNIAN-NORIAN BASIN-PLATFORM SYSTEM (JULIAN ALPS): CARBONATE PLATFORM PROGRADATION
Conclusions
After widespread Carnian drowning in the Julian Alps (and
also in the Kamnik—Savinja Alps more to the E) and the onset
of the Hallstatt type limestone sedimentation (Martuljek platy
limestone), rimmed prograding Dachstein platforms of the late
Tuvalian and early Norian appeared, filling newly-formed ba-
sins. The massive margin of the Dachstein platform is pre-
dominantly made of corals and sponges. The reef complex in
the Julian Alps attains a maximum thickness of 300 m, which
means that previous assumptions of the thickness were drasti-
cally exaggerated. Slope geometry, dip of clinostratification,
and age-dating of the basinal limestones indicate NE progra-
dation of the platform (in the recent orientation).
According to conodont dating, the Martuljek platy lime-
stone is successively younger in the NE direction and indi-
cates platform progradation with an estimated rate of 1200 m/
Myr. The conodont samples of the Martuljek platy limestones
yield abundant late Carnian—early Norian collections. In the
next phase of our study, bed-by-bed resampling is planned in
order to introduce precise conodont biozonation that would
enable identification of the boundary line. After definition of
the Carnian-Norian boundary and its ratification by interna-
tional geological institutions, the marking of the boundary
will also be possible.
There is currently no proof that the basin was connected
with true pelagic Hallstatt facies of the deep shelf bordering
the Meliata oceanic realm, although progradation indicates the
NE direction, which is away from the Slovenian Basin. The
Dachstein reef limestone in the Martuljek Mountain Group
and also in the Mt Triglav area is, based on the stratigraphy,
and on the relationship with well dated basinal limestones, of
the late Carnian to Norian age. The more than 1000 m thick
succession of the cyclic Dachstein Limestone of the Norian
and Rhaetian age sedimented in the broad peritidal area be-
hind the prograding reef.
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