Facies (2004) 50:77­105
DOI 10.1007/s10347-004-0004-y
O R I G I N A L A R T I C L E
Adam Tomaovch
Microfacies and depositional environment
of an Upper Triassic intra-platform carbonate basin:
the Fatric Unit of the West Carpathians (Slovakia)
Received: 4 April 2003 / Accepted: 18 January 2004 / Published online: 12 March 2004
 Springer-Verlag 2004
Abstract Facies associations of the Rhaetian Fatra For-
mation from the Vel·k Fatra Mts. (West Carpathians)
were deposited in a storm-dominated, shallow, intra-
platform basin with dominant carbonate deposition and
variable onshore peritidal and subtidal deposits, with 21
microfacies types supported by a cluster analysis. The
deposits are formed by bivalves, gastropods, brachiopods,
echinoderms, corals, foraminifers and red algae, ooids,
intraclasts and peloids. A typical feature is the consider-
able variation in horizontal direction. The relative abun-
dance and state of preservation of components as well
as the fabric and geometric criteria of deposits can be
correlated with depth/water energy-related environmental
gradients. Four facies associations corresponding to four
types of depositional settings were distinguished: a)
peritidal, b) shoreface, above fair-weather wave base
(FWWB), c) shallow subtidal, above normal storm wave
base and d) above maximum storm wave base. The
depositional environment can be characterized as a mo-
saic of low-relief peritidal flats and islands, shoreface
banks and bars, and shallow subtidal depressions. The
distribution and preservation of components were mainly
controlled by the position of base level (FWWB), storm
activity and differences in carbonate production between
settings. Poorly or moderately diverse level-bottom mac-
robenthic assemblages are dominated by molluscs and
brachiopods. The main site of patch-reef/biostrome car-
bonate production was located below the fair-weather
wave base. Patch-reef/biostrome assemblages are poorly
diverse and dominated by the branched scleractinian coral
Retiophyllia, forming locally dm-scale autochthonous ag-
gregations or more commonly parautochthonous assem-
blages with evidence of storm-reworking and substantial
bioerosion by microborings and boring bivalves.
Facies types and assemblages are comparable in some
aspects to those known from the Upper Triassic of the
Eastern and Southern Alps (Hochalm member of the
Kössen Formation or Calcare di Zu Formation), pointing
to similar intra-platform depositional conditions. The
absence of large-scale patch-reefs and poor diversity of
level-bottom and patch-reef/biostrome assemblages with
abundance of eurytopic taxa indicate high-stress/unstable
ecological conditions and more restricted position of the
Fatric intra-platform setting from the open ocean than the
intra-platform habitats in the Eastern or Southern Alps.
Key words Upper Triassic  Rhaetian  West
Carpathians  carbonate sedimentology  facies analysis 
benthic assemblages  coral patch-reefs
Introduction
The Upper Triassic epoch represents the start of the
modern coral-reef community type (Wood 1999) and the
onset of coral-zooxanthellae symbiosis (Stanley 1988;
Stanley and Swart 1995), the establishment of first Meso-
zoic epibiont communities (Lescinsky 2001), the ap-
pearance of abundant bivalve macroborers (Perry and
Bertling 2000), and the Norian and Rhaetian stages cor-
respond to the global reef bloom (Flügel 2002). However,
the end-Triassic mass extinction event represents a peri-
od of significant paleobiological and paleoenvironmental
change, when nearly 40% of invertebrate genera did not
survive into the Jurassic (Raup and Sep-koski 1982, 1986)
and reef ecosystems were affected by a significant drop
in the global carbonate production (Flügel and Kiessling
2002).
In the Fatric Unit of the West Carpathians, relatively
well-preserved Rhaetian-Hettangian marine successions
occur (Gadzicki et al. 1979; Michalík and Gadzicki 1983).
Although the precise position of the Rhaetian-Hettangian
boundary is questionable in these sections due to absence
of biostratigraphic-valuable taxa, the reconstruction of the
Rhaetian depositional environment of the Fatric Unit can
A. Tomaovch ())
Institut für Paläontologie, Würzburg Universität,
Pleicherwall 1, 97070 Würzburg, Germany
e-mail: adam.tomasovych@mail.uni-wuerzburg.de
Tel.: +49-931-312512
Fax: +49-931-31 25 04
be very useful in understanding the nature of pre-ex-
tinction benthic associations on local and regional scales.
Sedimentological features and paleontologic content of
the uppermost Triassic strata of the Fatric Unit are rel-
atively well-documented (Michalík 1973, 1974, 1977,
1979, 1980, 1982; Michalík and Jendrejkov 1978;
Gadzicki 1974, 1983), with some detailed information on
brachiopods (Michalík 1975), corals (Roniewicz and
Michalík 1991a, 1991 b, 1998), bivalves (Kochanov
1967; Gadzicki 1971) and vertebrates (Duffin and Gadz-
icki 1977). The results of these studies show a high
variation in the composition and preservation of the
deposits. However, detailed microfacies and paleoenvi-
ronmental analyses on a small-scale level are rare and
depositional models are mostly absent.
Paleoenvironmental reconstruction of the whole depo-
sitional setting of the Fatric Unit was performed by
Michalík (1977) who recognized ten facies areas on an
approximately 300-km-long transect through the West
Carpathians. The scale of observation in this study in-
cludes only a small portion of this intra-platform depo-
sitional setting, which is now preserved in a 25-km-long
transect in the Vel·k Fatra Mountains (central Slovakia).
This area is characterized by the presence of relatively
well-exposed sections and was therefore chosen for this
study.
The goals of this study are a) to define particular
microfacies types, based on 5 lithologic sections, their
spatial and temporal distribution and the relationship
between components, and b) to interpret of the deposi-
tional setting and its comparison with coeval settings on
the NW-Tethyan carbonate platforms. The first aspect is
necessary as it provides high-resolution framework for
understanding the horizontal facies variation. These de-
posits contain fossil assemblages with abundant taxa like
corals, bivalves and brachiopods that were substantially
affected by the end-Triassic extinction (Hallam 1996,
2002; Hallam and Wignall 1997) and can therefore
provide important information about distribution patterns
and habitats of these fossil groups at the end of the
Triassic.
Geologic Setting
During the Upper Triassic, the West Carpathians were
situated on the extensive epeiric carbonate platform on
the northwestern margin of the Tethys Ocean in the
subtropical climatic belt (Michalík 1994; Gawlick 2000)
(Fig. 1). The Upper Triassic carbonate platform of the
West Carpathians had been subdivided into several shore-
parallel depositional settings, now preserved in various
paleotectonic units. In a simplified scheme, the most
proximal nearshore zone was formed by extremely
shallow or continental deposits, followed seaward by
intra-platform mixed carbonate-siliciclastic or predomi-
nantly carbonate basins (this is the position of the Fatric
Unit), a Dachstein carbonate platform and finally rim-
ming Dachstein-reefs (Haas et al. 1995). The Rhaetian
Fatra Formation was deposited in a shallow-water intra-
platform, marine, predominantly carbonate setting of the
Fatric Unit (West Carpathians) (Michalík 1982) (Fig. 2).
Only in the southernmost part of the Fatric Unit de-
positional area, restricted peloidal bars/shoals of the
Svät Jakub Formation were deposited (Tomaovch and
Michalík 2000). In the Fatra Formation, the Rhaetian age
is confirmed by the first appearance of foraminifers
Triasina hantkeni and Glomospirella friedli (Gaz´dzicki
1983) and brachiopod Austrirhynchia cornigera.
Carbonate deposition took place under a low subsi-
dence regime. The proportion of siliciclastic admixture is
mostly very limited. The studied area of the Fatric Unit
was most probably connected with the Tethys Ocean
either via the shallow Dachstein platform top, or perhaps
through a system of deeper intra-platform basins formed
by the depositional settings of the Hronic (West Car-
pathians), Bajuvaric and Tirolic Unit (Eastern Alps). At
the beginning of the Jurassic, the depositional regime in
the Fatric Unit was abruptly replaced by the terrigenous
sedimentation of the Kopienec Formation (Hettangian-
Early Sinemurian, Fig. 2). In the overlie of the basal
clastic member of the Kopienec Formation, ammonites
Psiloceras psilonotum (Quenstedt) and Caloceras cf. torus
(d'Orbigny), equivalent to the Early Hettangian Psiloceras
planorbis Zone, were documented (Rakffls 1993). There-
fore, the age of lowermost part of the Kopienec Formation,
Fig. 1 General paleogeographic position of the Fatric Unit (Central
West Carpathians) in the Upper Triassic (Norian/Rhaetian). After
Michalík (1994), modified
78
formed by approximately 5- to 20-m-thick barren silt-
stones/claystones, is unknown.
Methods
The database includes 5 stratigraphic key sections of the Fatra
Formation (Figs. 3, 4, 7, 10). In addition, 8 sections exposing only
parts of the Fatra Formation were studied for comparative purposes
(Fig. 3). Sedimentologic, taphonomic and paleobiologic features
at the bed level were described in the field. Sections have been
measured bed-by-bed and numbered from bottom to top. Samples
for thin sections have been obtained from 2-m-distant intervals. In
addition, denser sampling of up to 20-cm-distant intervals was
performed in segments which exhibit high facies variation. In the
lower part of Dedoova ­ Frèkov locality, several parallel sections
were measured in horizontal direction in order to map a spatial
variation of the patch reef/biostrome facies (Fig. 15A). The textural
classification of Dunham (1962) and Embry and Klovan (1972) was
used with modifications for the description of microfacies types.
The term "biostrome" is used for dm-scale, sheet-like autoch-
thonous or parautochthonous deposits with relatively high propor-
tion of constructors, bafflers and binders (corals, algae and/or
sponges). The term "patch-reef" is used for meter-scale, mound-
Fig. 2 Basic lithostratigraphic scheme of the uppermost Triassic-
lowermost Jurassic strata in the Fatric Unit, Central West Carpathi-
ans. The subdivision of the Fatra Formation into four intervals
corresponds to four large-scale sequences bounded by three
unconformities
Fig. 3 A. Overview map with the study area. B. Geographic
location of studied lithologic sections of the Fatra Formation in the
Vel·k Fatra Mts., Slovakia. 1 ­ Dedoova, 2 ­ Sviniarka, 3 ­
Belianska-Boriov, 4 - Bystr potok, 5 ­ Rztoky, 6 ­ Krína, 7 ­
Revfflcky Mlyn, 8 - Balcierovo, 9 ­ Boriov-farm, 10 ­ Mal
Ramin, 11 ­ arnovka, 12 - Zelen-Brnovsk, 13 ­ oproò
79
like or flat-topped deposits consisting of autochthonous or pa-
rautochthonous remains of constructors, bafflers and binders that
can be composed of several stacked biostromes. All together, 209
thin sections were studied. Relative abundance of 14 components
(bivalves, gastropods, brachiopods, echinoderms, ostracods, corals,
calcareous sponges, red algae, green algae, foraminifers, sessile
foraminifers, ooids, intraclasts, and peloids) was estimated using
comparative chart method of Bacelle and Bosellini (1965) and
Schäfer (1969). These quantitative data formed the basis of a data
matrix for a Q-mode cluster analysis using the squared Euclidean
distance and the Ward method as the clustering technique (see
Appendix). Individual clusters were named after the dominating
components.
As the composition of samples is described by percentage
values that represent dependent parts (Reyment and Savazzi 1999),
standard exploratory multivariate techniques prone to the unit-sum
constraint (e.g. PCA) cannot be used. In order to reduce the overall
complexity of the data by extracting hypothetical variables (di-
mensions) accounting for the maximum correlation between sample
and component scores, correspondence analysis can be used for
percentage data (Kowalewski et al. 2002). Correspondence analysis
allows observing the simultaneous representation of samples and
taxa within the same system of coordinate axes. The arch effect and
compression of the ends of the gradient were eliminated by
applying a detrended correspondence analysis (DCA, Hill and
Gauch 1980).
In order to decrease data heterogeneity and exclude outliers,
samples with allochem content below 10% were excluded from
data analysis. This data matrix (exhaustive data set) for DCA
comprises 14 components as variables and 152 thin sections as
objects. In order to see a primary ecological relationship between
individual organism groups, the data matrix was minimized by
excluding microfacies types with evidence of high alteration (high-
proportion fragmentation, disarticulation and abrasion) and trans-
port/reworking (good sorting, presence of intraclast and ooids).
This data matrix (reduced data set) for DCA contains 11 bioclast
types and 78 thin sections as the objects. The reduced data set
contains seven microfacies types (MF 4 - bio-wackestone, MF 5 -
brachiopod floatstone, MF 6 - gastropod floatstones/packstone, MF
7 - solenoporacean framestone, MF 8 - coral framestone, MF 9 -
bio-floatstone with micritized corals and MF 18 - bivalve float-
stone).
Results
Sections
Five lithologic sections of the Fatra Formation are
presented in Figures 4, 7­10. The meter-scale spatial
variation in coral patch-reef/biostrome facies types in
Dedoova-Frèkov section is shown in Fig. 15A. As the
Fatra Formation in the Vel·k Fatra Mts. can be subdi-
vided into four main intervals (large-scale sequences)
bounded by laterally extensive unconformities (Tomao-
Fig. 4 Lithologic section of the Fatra Formation in Dedoova -
Frèkov. Explanations: See Fig. 8
Fig. 5 Coral patch-reef/biostrome facies types: 1. Massive coral
Astraeomorpha sp., strongly bored with bivalves (1), and encrusted
by oysters (2). Some free spaces are occupied by small terebratulids
(3). Sample DD4.4. Scale: 1 cm 2. Coral colony of Retiophyllia
paraclathrata, with terebratulid Rhaetina gregaria (arrow) between
corallites. Sample S82. Scale: 1 cm 3. Small branching bush-shaped
solenoporacean alga, bored with bivalves (arrow). Sample DD5.2.
Scale: 1 cm 4. Stacked, 10­20 cm thick coral colonies of
Retiophyllia gosaviensis. Dedoova ­ Frèkov A (beds 4.15­4.18).
Scale: 10 cm 5. Toppled coral colony of Retiophyllia gosaviensis.
Dedoova ­ Frèkov E (bed 5). Scale: 10 cm
80
81
82
vch 2002), the following description of the sections is
based on this subdivision. The correlation of the first
large-scale sequence and spatial variation of coral-patch
reef/biostrome facies types on km-scale is presented in
Figure 15B.
1. Dedoova ­ Frèkov (Fig. 4) represent outcrops in the
forest which are situated on the steep SW slope of the
Frèkov hill (1585 m), in the closure of the Dedoova
dolina valley, NW of the Krína (1574 m). The Fatra
Formation is completely exposed together with upper-
most part of the underlying "Carpathian Keuper
Formation". The upper boundary is observable only
at some places because of tectonization and weathering
of the basal siltstones and claystones of the Kopienec
Formation.
In the lowermost 11.5 m thick interval of the Fa-
tra Formation (1st
large-scale sequence), small-scale
coarsening-upward sequences are preserved (beds 1­
3). Limestones are characterized by a complex internal
structure formed by cm-scale alternation of poorly
sorted floatstones with well-preserved bivalves (Pla-
cunopsis alpina, Atreta intusstriata, Chlamys valonien-
sis) and well-sorted packstones/grainstones with ero-
sional bases and poorly preserved bioclasts. These
beds are abruptly replaced by brachiopod floatstones
with Rhaetina gregaria and bioclastic packstones with
bivalve, echinoderm, brachiopod and coral fragments
(bed 4). In detail, horizontal and vertical distribution of
individual facies types and benthic taxa is variable in
this part of the section (Fig. 4). Locally, isolated coral
colonies of massive (Astraeomorpha) and branching
(Retiophyllia) corals or solenoporacean algae are
present in life or overturned/toppled position (Fig.5­
5) and form meter-scale aggregations. Both massive
and branching corals and algae in these beds are
strongly encrusted with oysters (Atreta) and bored by
bivalves (Fig.5­1, 3, Fig.6­6, 7). Upwards, they are
replaced by a 2-m-thick patch-reef/biostrome complex
formed by coral framestones with complete colonies of
Retiophyllia gosaviensis (beds 5­6) with rare interca-
lations of intraclastic limestones. 10­50 cm high fan or
dome-shaped Retiophyllia coral colonies, with diam-
eters between 20 and 100 cm (Fig. 5­4), are still
preserved in growth position, with corallites (5­10 mm
in diameter) radiating in upward direction. The pro-
portion of borings and encrustations is relatively low.
Fig. 7 Lithologic section of the Fatra Formation in Sviniarka ­
Mal Zvolen valley. The section is tectonically disrupted. Expla-
nations: See Fig. 8
Fig. 6 Shallow subtidal facies types, above normal storm wave
base: 1. Gastropod packstone with foraminifers and algae (MF 6).
Sample DD7.7. Scale: 5 mm 2. Framestone with solenoporaceans
(MF 7). Sample DD5.2. Scale: 5 mm 3. Coral framestone (MF 8)
with Retiophyllia gosaviensis (corallites with local dark automi-
critic coatings and encrusting bivalve - arrow). Sample DD5.12.
Scale: 5 mm 4. Floatstone with micritized corals (MF 9) containg
R. paraclathrata and abundant involutinid foraminifers. Sample
DD19.2. Scale: 5 mm 5. Floatstone with micritized corals (MF 9)
(R. paraclathrata with bioerosions and encrustations of Baccinella
sp. and Lithocodium sp. and calcareous sponge). Sample DD18.10.
Scale: 5 mm 6. Bivalve macroboring with recrystallized valves in
the retiophyllid coral (MF 9). Sample DD5.8. Scale: 1 mm 7.
Bivalve macroboring in solenoporacean alga (MF 7). Sample
DD5.2. Scale: 1 mm 8. Bacinella sp., boring and encrusting
recrystallized coral fragment (MF 9). Sample DD18.10. Scale:
1 mm
83
Coral framestones are capped by laminated bindstones
with an erosional unconformity at the top.
In the middle 9.7-m-thick interval (2nd
large-scale
sequence), thick packstones with intraclasts occur
(bed 7), passing upwards into gastropod floatstones
(bed 8) and capped by laminated bindstones (bed 11),
at the top with an erosional unconformity with well
sorted grainstone (bed 12). Above this unconformity,
a 14.7-m-thick interval (3rd
large-scale sequence) con-
sisting of dolomites with fenestral pores and sheet
cracks and well- or bimodally sorted grainstones,
packstones and rudstones with brachiopods, bivalves
and gastropods is preserved (beds 14­18), passing into
brachiopod floatstones (bed 16), ooidic packstones
(bed 17) and well-sorted intraclastic grainstone (bed
18). Upwards, bioclastic floatstones with Retiophyllia
coral fragments (beds 19­20) are capped by laminated
bindstones (bed 24).
In the uppermost 2.7 m thick interval of the Fatra
Formation (4th
large-scale sequence), bioclastic pack-
stones and rudstones with bivalves (Rhaetavicula con-
torta, Placunopsis alpina, Chlamys sp., Modiolus min-
utus, Palaeocardita austriaca) and bioclastic-oolitic
limestones with calcitic, chamositic and ferrigenous
ooids, and coral, echinoderm, bivalve and brachiopod
(Rhaetina gregaria) fragments are preserved. Isolated
coral colonies (Retiophyllia sp.) are locally present.
2. Svinarka - Mal Zvolen (Fig. 7) represent outcrops in
the creek in the Svinarka valley and smaller exposures
in the forest east of the creek, SE of the Mal Zvolen
hill (1372 m). In the creek, the lower and upper
boundary of the Fatra Formation is exposed; the
middle part is tectonically disrupted. The correlation
with the forest exposures allowed to discern a com-
plete stratigraphic column of the Fatra Formation at
this locality. In the lowermost, 9.4-m-thick interval of
the Fatra Formation (1st
large-scale sequence), metre-
scale coarsening-upward sequences prevail, consisting
of dark claystones, coquinal floatstones with bivalves
(Rhaetavicula contorta, Placunopsis alpina) and well-
sorted packstones/grainstones (beds 77­79). These
beds pass into coquinal floatstones with abundant
brachiopods (Rhaetina gregaria, Zugmayerella unci-
nata) and bivalves (Plagiostoma punctatum, Modiolus
minutus, Pteria sp., Antiquilima sp., Atreta intusstri-
ata, Chlamys sp.) (beds 80­81) and small dm-scale
coral framestones with Retiophyllia paraclathrata (bed
82, Fig. 5­2). Here, 30- to 40-cm-high coral colonies
with corallites 5 mm in diameter are mostly toppled.
These beds are overlain by fenestral and cryptalgal
bindstones with a capping erosional unconformity. In
the middle 12-m-thick interval of the Fatra Formation
(2nd
large-scale sequence), thick-bedded bioclastic and
gastropod limestones are preserved, capped by lami-
nated limestone with rip-up clasts, fenestral pores
and sheet cracks (bed 87). In the upper 11.5-m-thick
interval (3rd
large-scale sequence) consisting of ooidic
grainstones and packstones, bio-rudstones and crinoid
floatstones is present (beds 88­96), capped by mud-
stones and dolomudstones (beds 97­98) with an un-
conformity at the top. In the uppermost, about 3-m-
thick interval of the Fatra Formation (4th
large-scale
sequence), rudstones, grainstones and packstones with
micritized bivalves, echinoderms and coral fragments
are preserved. Biomicritic wackestone with in-situ
corals is present as a 15-cm-thick interbed. The up-
permost bed of the Fatra Formation is formed by well-
sorted grainstone with strongly micritized bivalves and
crinoids.
3. Belianska ­ Boriov (Fig. 8) represent exposures in the
forest pathway leading from the Havranovo to the
cottage below Boriov hill, 300 m below the cottage,
east of the Boriov hill (1509 m). The upper part of the
"Carpathian Keuper Formation" and lower and middle
parts of the Fatra Formation are exposed here. The
uppermost part of the "Carpathian Keuper Formation"
is formed by light grey thick-bedded dolomudstones.
In the first large-scale sequence of the Fatra Formation
(12 m), small-scale shallowing-upward sequences
occur (beds 1­11). In their lower part, they are formed
by bioclastic limestones with complex internal strat-
ification (mm- or cm-scale alternation of floatstones
with packstones) and bivalves (Bakevellia praecursor,
Placunopsis alpina) and laminated mudstones (beds
1­6). In their upper part, bioclastic floatstones are
replaced by well-sorted packstones/grainstones (beds
7­10). Upwards, these beds pass into bioclastic wacke-
stones/floatstones with brachiopods (beds 13­15) and
higher-up into well sorted packstones and grainstones
with erosional boundaries (beds 16­17). These are
overlain by thick packstones/floatstone with coral
fragments and intraclasts (bed 18). In the middle
6-m-thick interval (2nd
large-scale sequence), laminat-
ed dolomites are capped by an erosional unconformity,
with well sorted packstones (bed 23). Up-section,
brachiopod floatstones with internal stratification,
well-sorted packstones and oo-grainstones are pre-
served (beds 27­30).
4. 4. Bystr potok ­ Ruomberok (Fig. 9) represent ex-
posures in the road cut from Ruomberok to Martin,
between the village È ernov and Hubov, near the
entry of the Bystr potok creek into the Vh River. The
locality had been mentioned by Stur (1859) and
partially described by Michalík (1985) and Tomao-
vch (2000). The middle and upper part of the Fatra
Formation are exposed. In the lower part of the section
(7.5 m), two shallowing-upward sequences capped by
laminated mudstones/bindstones are preserved (beds
1­6). The second one is capped by an unconformity
and overlain by well-sorted packstones with intraclasts
and micritized bioclasts. This forms the base of a
coarsening-upward sequence and passes upward into
thick packstones with megalodonts, brachiopods, al-
gae, coral fragments and echinoderms and oobio-
grainstones at the top (beds 7­9). In the middle part
of the section (4 m), alternation of coquinal lime-
stones with marls with abundant brachiopods (Rhae-
tina gregaria, Zugmayerella uncinata, Austrirhynchia
84
cornigera, Discinisca suessi) and bivalves (Actinos-
treon haidingerianum, Atreta intustriata, Modiolus
minutus, Plagiostoma punctatum, Chlamys sp., An-
tiquilima sp., Pteria sp., Liostrea sp.) occur (beds 9­
10). They pass into dm-scale alternations of packstones
with mudstones (beds 11­16). In the upper part of the
section (3.7 m), packstones and grainstones with ooids,
intraclasts and bioclasts prevail (beds 18­23), passing
into dolomitic mudstones in the uppermost part of the
section.
5. Rztoky ­ Nolèovo (Fig. 10) represents exposures
which are situated in the forest pathway on the left
slope of the valley above the Rztoky creek, south of
the Ostr hill (786 m), above the Nolèovsk dolina
valley. This section was described by Michalík and
Skora (1979). In the first large-scale sequence of the
Fatra Formation (12 m), metre-scale shallowing-up-
ward sequences (beds 1­3) are overlain by brachiopod
and crinoid floatstones (beds 4­7). Higher, a coral
limestone with Retiophyllia (bed 8) passes into thick
grainstones and packstones (beds 9­10). In the second
large-scale sequence of the Fatra Formation (11.5 m),
an alternation of dolomites with bioclastic limestones
is preserved, finally capped by laminites with an
erosional unconformity at the top (beds 21­22). In the
third large-scale sequence (11.5 m), three small-scale
shallowing-upward sequences occur (beds 32­40).
They consist of laminated limestones with foraminifers
and ostracods, well-sorted intraclastic grainstones, co-
quinal floatstones with brachiopods (Rhaetina gre-
garia, R. pyriformis) and floatstones with bored/en-
crusted coral fragments (Retiophyllia paraclathrata)
and are capped by a dolomite (bed 40). In the up-
permost, fourth large-scale sequence, about 1 m of
mudstone interval (bed 45) is overlain by floatstones
with abundant megalodonts, gastropods and foramini-
Fig. 9 Lithologic section of the Fatra Formation at the Bystr
potok locality near Ruomberok. Explanations: See Fig. 8
Fig. 8 Lithologic section of the Fatra Formation in Belianska-
Boriov
85
fers. The uppermost bed of the Fatra Formation is
formed by coquinal biointra-rudstone with well-sorted,
concordantly oriented and strongly micritized frag-
ments of bivalves, brachiopods and echinoderms (bed
48).
Microfacies types
In the Q-mode cluster analysis performed at the sample
level and based on relative frequencies of components, 20
cluster types have been recognized (see Appendix).
However, the final distinction of microfacies types was
also based on fabric criteria (sorting, packing and orien-
tation), bed geometry and internal stratification and does
not strictly reflect the results of the cluster analysis.
Therefore, some clusters were subdivided and all together
21 microfacies types are described in the following part.
The samples within the first cluster were subdivided into
mudstones (MF 1) and laminated bindstones (MF 3).
Clusters 7 and 8 were fused in one MF type (MF 9 - bio-
floatstone with micritized corals). Clusters 9­11 were
assigned to MF 10 and 12 according to the dominating
size of components. In spite of the drawbacks due to
subjective assignment of some samples, it is suggested
that a cluster analysis can be useful as a first step in
microfacies types demarcation in settings with high facies
variation. Mean values with standard deviations of rel-
ative abundances of components are summarized for
each microfacies type in histograms (Fig. 11). The DCA
ordination of the exhaustive and reduced data set is shown
in Fig. 16.
MF 1 ­ Mudstone
This type (Fig. 12­2) is represented by light grey, thick-
bedded (25­60 cm) dolomudstones and dolomitized
mudstones, spatially associated with laminites or intra-
clastic limestones. They often display fenestral fabric and
internal sediment filling. Fenestral pores form discontin-
uous, concordant, irregularly-shaped sparitic laminae,
locally passing into continuous sheet cracks. In some
beds, agglutinated foraminifers (Glomospirella), ostra-
cods and calcarenous green algae (Halicoryne) are com-
mon.
MF 2 ­ Intraclastic breccia (floatstone)
This facies type (Fig. 12­1) is characterized by a
bioturbated matrix and dark angular and irregular micritic
intraclasts (several mm to 2­3 cm). Fenestral pores with
internal sediment may be locally present. Ostracod shells
and disarticulated valves may occur, along with small
fragments of echinoderms and bivalves.
Fig. 10 Lithologic section of the Fatra Formation in Rztoky -
Nolèovo. Explanations: See Fig. 8
86
Fig. 11 Histograms of microfacies types showing mean values and
standard deviations of individual components. The first three
microfacies types are not shown because of rare or absent
components. Explanations: 1­Bivalves, 2­Gastropods, 3­Bra-
chiopods, 4­Echinoderms, 5­Ostracods, 6­Corals, 7­Calcareous
sponges, 8­Ooids, 9­Intraclasts, 10­Peloids, 11­Foraminifers, 12­
Sessile foraminifers, 13­Micritized bioclasts, 14­Green algae, 15­
Red algae, 16­Microbialites
87
Fig. 12 Peritidal facies types: 1. Intraclastic breccia (MF 2).
Sample S87. Scale: 5 mm 2. Mudstone with foraminifers (Glomo-
spirella) (MF 1). Sample R32. Scale: 1 mm 3. Cryptalgal bind-
stone (MF 3). Sample DD11. Scale: 1 mm 4. Pel-packstone with
foraminifers (MF 14). Sample BP5. Scale: 1 mm 5. Fenestral
bindstone (MF 3). Sample NR8. Scale: 5 mm 6. Fenestral bindstone
(MF 3). Sample S11.2. Scale: 5 mm 7. Fenestral bindstone (MF 3).
Sample NR8. Scale: 5 cm
88
MF 3 ­ Laminated bindstone
1. Fenestral bindstone (Fig. 12­5­7) with millimetre-scale
wavy horizontal lamination formed by micritic laminae
and more or less continuous or discontinuous fenestral
sparitic laminae with irregular lower and upper bound-
aries.
2. Cryptalgal bindstone (Fig. 12­3) with finely or
moderately crinkled horizontal lamination consisting of
alternation of calcilutitic laminae and very well-sorted
calcisiltic bioclastic-microintraclastic laminae, locally
with micrograding.
3. Planar or low-angle cross-stratified, mm-scale lam-
ination formed by less regular alternation of micritic
laminae with dispersed bioclastic debris and calcisiltic to
calcarenitic laminae with densely packed fragments of
foraminifers, bivalves and crinoids, often with concordant
orientation.
MF 4 ­ Bio-wackestone
This type shows the presence of moderately sorted,
ran-domly oriented, and mostly poorly preserved bi-
valve fragments, gastropods, echinoderm ossicles and
brachiopods. Complete macroscopic remains are very
scarce. Microfossils are represented by ostracods, no-
dosariid and glomospirellid foraminifers, globochaetes,
dasycladacean algae (Halicoryne) and holothurian scle-
rites.
MF 5 ­ Brachiopod floatstone/packstone
This type (Fig. 13­7) is preserved in dark grey, thin-
bedded (5­25 cm) limestone beds. It commonly displays
bioturbated and pelletized micritic matrix and contains
predominantly well-preserved terebratulid brachiopods
(Rhaetina gregaria), with very rare traces of micritization
or bioerosion. In some beds, shells with geopetal infillings
are frequent. The biofabric is dispersed or loosely packed,
less commonly densely packed, with poor sorting and
mostly random orientation of brachiopods.
Fragments of bivalves, crinoid ossicles, echinoid
spines, juvenile gastropods, ostracods and sessile for-
aminifers are common. Nodosariid, glomospirellid and
trochamminid foraminifers, serpulids, corals, cyanobac-
teria (Cayeuxia) and fragments of calcareous red (Soleno-
poraceae) or green (Codiaceae) algae may be locally
present. In some cases, stratification formed by alterna-
tion of brachiopod floatstones with 5­10 mm thick,
redeposited, well-sorted, calcarenitic laminae with basal
erosional surfaces is recognizable.
MF 6 ­ Gastropod floatstone/packstone
This type (Fig. 6­1) is dominated by poorly/moderately
sorted, non-micritized, well-preserved, complete or frag-
mented gastropods (5­30%), usually with geopetal struc-
tures. Involutinid (Aulotortus communis and A. tumidus),
glomospirellid and nodosariid (Frondicularia woodwardi)
foraminifers (2.5­10%), green calcareous algae (Codi-
aceae), cyanobacteria (Cayeuxia), bioeroded and mi-
critized fragments of megalodonts and other bivalves
and fragmented or complete, non-micritized echinoderm
ossicles are common. The microfossils are additionally
represented by Halicoryne, Globochaete, ostracods and
ophiuroid fragments, and microproblematic Earlandia
(Flügel 1972; Borza 1975).
MF 7 ­ Solenoporacean framestone
It forms dark grey, 20­50 cm thick lensoidal patches
in the limestone beds in the lower part of the Fatra
Formation (Dedoova-Frèkov and Krína). This type (Fig.
5­2, Fig. 6­2) contains predominantly well-preserved
solenoporacean algae that are not affected by fragmen-
tation and micritization. They are often bored by bivalves
and endolithic microborers (Fig. 6­7). Apart from red
algae, the diversity of frame builders is very poor,
calcareous sponges are only locally present. Brachiopods,
bivalves and crinoid ossicles are commonly dispersed in
the matrix in the interspaces between algae.
MF 8 - Coral framestone
This type is characterized by the dominance of branching
corals (Retiophyllia gosaviensis, R. paraclathrata, and R.
fenestrata) which represent primary framework builders
(Fig. 6­3). They are commonly encrusted by oysters (Fig.
6­3), calcareous sponges, sessile foraminifers and ser-
pulids. In the micritic matrix, fragments of brachiopods,
bivalves, crinoids, algae, ostracods and microbial intra-
clasts and peloids are commonly dispersed in spaces
between corals. Tabular corals (Astraeomorpha) are rare,
forming only locally small-scale, 30­50 cm thick mono-
typic aggregations. Two basic types of micritic matrix are
present. The more common is gravity-controlled allomi-
crite, it has a grey colour and locally unhomogenous
structure (pelletized or bioturbated) in thin sections. It
forms infillings of cavities and interspaces between com-
ponents. The second type is represented by automicrite,
which includes gravity-defying deposits in the form of
coatings, crusts, layers on the surfaces and in the internal
cavities of bioclasts. In the thin sections, automicritic
coatings are dark brown to black, homogenous and most-
ly structureless. Allochems are absent in these gravity-
defying automicritic coatings, in contrast to allomicritic
type with diverse assemblage of bioclasts.
MF 9 ­ Bio-floatstone with micritized corals
This type is characterized by the presence of degraded
retiophyllid corals (Fig. 6­4, 5, 6). Bioclasts are randomly
89
Fig. 13 Shallow subtidal facies types, above normal storm wave
base: 1. Floatstone with micritized bioclasts (MF 19). Sample
DD2.7. Scale: 5 mm 2. Floatstone with micritized bioclasts (MF
19). Sample B12. Scale: 5 mm 3. Packstone/wackestone with
micritized bioclasts (MF 20). Sample DD5. Scale: 5 mm 4.
Packstone/wackestone with micritized bioclasts (MF 20). Sample
DD5.3. Scale: 5 mm 5. Storm-reworked deposit ­ in the basal part
with bivalve floatstone (MF 18), in the upper part with bio-rudstone
(MF 10). Sample K2.10. Scale: 5 mm 6. Packstone/wackestone
with micritized bioclasts (MF 20). Sample DD5a. Scale: 5 mm 7.
Brachiopod floatstone (MF 5). Sample DD4.2. Scale: 5 mm
90
oriented and poorly sorted. Fragments of coral colonies or
isolated corallites (Retiophyllia paraclathrata) are com-
monly strongly destructively micritized, microbored and
encrusted (common sessile foraminifers, Thaumatoporel-
la sp., Baccinella, Lithocodium, (Fig. 6­8), cf. Ko³odziej
1997) and/or covered with automicritic coatings. Bi-
valve macroborings are common (Fig. 5­1, Fig. 6­6).
Calcareous (nodosariids, involutinids, Ophthalmidium)
and agglutinated (Glomospirella, Trochammina, Tetra-
taxis) foraminifers, ostracods, globochaetes, cyanobac-
teria (Cayeuxia sp.), sponges, fragments of bivalves,
gastropods, brachiopods and echinoderm ossicles are
common.
MF 10 ­ Well-sorted bio-rudstone
with micritized bioclasts
10­40 cm thick beds of this type commonly display good
sorting, dense packing and concordant, edgewise/nested
or random orientation of bioclasts (Fig. 14­7, 8). Grading
in the proportion of matrix and size and density of
allochems is locally preserved. High proportions of frag-
ments of bivalves, echinoderms, gastropods and bra-
chiopods are degraded (abraded, micritized and bioerod-
ed). In several cases, certain proportions of bioclasts are,
in contrast, relatively well preserved, without traces of
bioerosion and abrasion. Encrustations by sessile forami-
nifers are rare.
MF 11 ­ Bimodally sorted bio-rudstone/grainstone
with micritized bioclasts
This type (Fig. 14­5, 6) consists of concordantly oriented,
convex-up bivalves with drusy sparitic shelters and local
mud-infiltrations, and well-sorted calcarenitic debris (up
to 2 mm). Rudite-size bivalve fragments with micritic
rims are mostly encrusted by sessile foraminifers, bored
and abraded. Bio- and oomicritic intraclasts, peloids
and radial ooids (with fragments of bivalves, crinoids,
foraminifers and peloids as nuclei) are common.
MF 12 ­ Bio-grainstone with micritized bioclasts
This type (Fig. 14­2) is characterized by well-sorted and
densely packed fabric, only locally with micrite, and
usually contains abraded, fragmented and strongly bio-
eroded bioclasts with micritic rims and sessile foramini-
fers (Tolypammina, Planiinvoluta). Debris of bivalves,
gastropods with exotic micritic infillings, echinoderm
ossicles (locally with syntaxial rims) and brachiopods are
abundant. Fragments of corals and calcareous algae can
occur locally. Bio- and oomicritic intraclasts, peloids and
radial ooids are present.
MF 13 ­ Oo-grainstone
10­50 cm thick beds of this type are characterized by
good sorting of ooids (approximate diameter: 1­1.5 mm),
with oval, circular or elongate outline and radial structure
showing several cortical layers (Fig. 14­1). Intraclasts
and micritized and abraded bioclasts are less common
(2.5­5%). Ooid nuclei consist of recrystallized bivalve
fragments, brachiopods, crinoids, foraminifers, micritic
and biomicritic intraclasts or peloids.
MF 14 ­ Pel-packstone
This type (Fig. 12­4) is characterized by the dominant
presence of well-sorted peloids (maximum size 1 mm)
and agglutinated foraminifers (Glomospirella), and less
common fragments of echinoderms, micritized bivalves,
and ostracods.
MF 15 ­ Intra-packstone
This facies type typically occurs in dark grey massive and
thick-bedded limestones (50­200 cm) in the middle part
of the Fatra Formation. They display bimodal sorting
consisting of well-sorted intraclastic-peloidal debris and
poorly sorted rudite-size bioclasts, with no preferred
orientation. A micritic matrix may be locally absent.
Ooids can also be present. Bioclasts are abraded, en-
crusted (Tolypammina, Planinvoluta, Thaumatoporella)
and bored/micritized (endolithic microborings). Some
bioclasts are in contrast relatively well preserved without
signs of bioerosion and abrasion. Recrystallized bivalve
fragments are dominant, gastropods, corallite fragments
or fragments of coral colonies and solenoporacean algae,
echinoderm ossicles and brachiopod valves are common.
The microfauna is characterized by a relatively diverse
assemblage of foraminifers (Triasina hantkeni, Tetra-
taxis inflata, Trochammina alpina, Frondicularia wood-
wardi, Glomospirella), globochaetes, Earlandia, green
algae (Halicoryne), and ostracods.
MF 16 ­ Oobio-packstone
Beds of this type contain calcarenitic debris with abun-
dant well-sorted ooids (0.5­1 mm) with radial structure
and oval outline. The ooid nuclei are formed by fragments
of bivalves, crinoids, intraclasts or peloids. Micritized
bivalve fragments and micritic intraclasts are common;
gastropods, brachiopod fragments, echinoderm ossicles
and green algae (Halicoryne) are present in varying pro-
portions. In general, bioclasts are mostly poorly pre-
served. In one subtype, components (1­1.5 mm) com-
pletely encrusted by sessile foraminifers (Tolypammina)
are very common.
91
92
MF 17 ­ Intrabio-packstone/grainstone
Beds of this type usually display a basal erosional surface,
good sorting (below 1 mm) and dense packing of angular
or oval microintraclasts and micritized/bored or abraded
bioclasts (bivalves, echinoderms). Calcareous (Triasina,
Aulotortus) and agglutinated (Glomospirella) foramini-
fers, globochaetes, green algae (Halicoryne) and thick-
shelled ostracods are locally abundant. Mostly they occur
in the direct overlie of mudstones (MF 1) or laminites
(MF 3).
MF 18 ­ Bivalve floatstone
Dark grey, 5­10 cm thick beds of this type (Fig. 13­5)
commonly alternate with 1­10 cm thick bio-floatstones
(MF 19) or bio-wackestones/packstones with micritized
bioclasts (MF 20). They contain poorly sorted and dis-
persed/loosely packed, complete or fragmented bivalves
(Placunopsis alpina, Rhaetavicula contorta, Bakevel-
lia praecursor, Gervillaria inflata, Chlamys valoniensis),
mostly randomly or less commonly concordantly oriented/
nested. Sparitic shelters or geopetal textures are scarce or
absent. Valves are commonly encrusted by sessile for-
aminifers. However, the proportion of bioerosion and mi-
critization due to activity of microborers is much lower in
comparison to floatstones and wackestones/packstones of
the MF 22 and 23.
MF 19 ­ Bio-floatstone with micritized bioclasts
5­20 cm thick beds of this type are characterized by the
abundance of bivalves and high degree of destructive
micritization and bioerosion (Fig. 13­1, 2). They are
usually associated with a complex internal structure
consisting of alternation of thin cm-scale intervals with
different sorting and packing density. Internal erosional
surfaces are locally present. The typical feature is a
loosely/densely packed bio-fabric, poor or moderate
sorting (with maximum size mostly not exceeding 10­
20 mm), and concordant (both convex-up and down),
nested or random orientation of bivalves, locally with
sparitic shelters under convex-up valves. Other compo-
nents are represented by micritic intraclasts and radial
ooids. Ooids are frequently encrusted by sessile forami-
nifers.
MF 20 ­ Bio-wackestone/packstone
with micritized bioclasts
This type is characterized by moderate or good sorting
and loose/dense packing of bioclasts, mostly dominated
by bivalves (Fig. 13­3, 4, 6, Fig. 14­3, 4) and by a
complex internal microstratigraphy. In the fossil assem-
blages characterized by high degree of taphonomic
alternation, fragments of recrystallized bivalves, echino-
derm ossicles (sometimes with syntaxial rims), juvenile
gastropods, corals, solenoporacean red algae and bra-
chiopods are abundant. In general, micritic rims are very
common. The microfauna is represented by sessile (Toly-
pammina), nodosariid or glomospirellid foraminifers,
serpulids, green algae (Acicularia), globochaetes (Globo-
chaete alpina, G. tatrica) and ostracods.
MF 21 ­ Crinoid wackestone/packstone
This type is characterized by the abundance of complete
or fragmented crinoid ossicles, locally still articulated,
with microborings and locally with micritic envelopes.
The biofabric is densely/loosely packed and moderately
sorted. Fragments of brachiopods, bivalves, ostracods,
echinoid spines are less common.
Discussion
Facies interpretation
In the following discussion , particular microfacies types
are interpreted in terms of paleoenvironment and com-
pared with coeval facies types known from other
Upper Triassic Tethyan carbonate settings. Fenestral and
cryptalgal bindstones (MF 3) can be interpreted as algal
or microbial mat deposits that are typical mainly of
peritidal flats (Shinn 1983). In the Upper Triassic car-
bonate environments, they typically represent an intertidal
member of the Lofer sequences (Schwarzacher 1948;
Fischer 1964; Flügel 1981; Enos and Samankassou 1998).
In addition, they commonly occur in shallow restricted
lagoonal settings of the Kössen and Calcare di Zu
Formation (Kuss 1983; Lakew 1990). Fenestral fabric is
mainly formed by desiccation and shrinkage or air and
gas bubble formation, and is often preserved within
stromatolites due to irregular growth processes (Shinn
1968). Algal mat lamination is not limited only to supra-
intertidal environment, but it is mostly not preserved due
to bioturbation and gastropod grazing in subtidal envi-
ronments (Garrett 1970), although it may be preserved in
a hypersaline environment. The absence of bioturbation
and body fossil fauna thus indicates unfavourable condi-
tions for metazoan life. Regular, mm-scale alternation of
Fig. 14 Shallow subtidal - nearshore facies types (above fair-
weather wave base): 1. Oo-grainstone (MF 13). Sample S92.3.
Scale: 1 mm 2. Bio-grainstone with micritized bioclasts (MF 12).
Sample DD5.1. Scale: 5 mm 3. Bio-packstone with micritized
bioclasts (MF 20). Sample DD 13.5. Scale: 5 mm 4. Bio-packstone
with micritized bioclasts (MF 20). Sample DD17.2. Scale: 5 mm 5.
Bimodally sorted rudstone/grainstone with micritized bioclasts (MF
11). Sample B7.3. Scale: 5 mm 6. Bimodally sorted rudstone/
grainstone with micritized bioclasts (MF 11). Sample DD15.5.
Scale: 5 mm 7. Bio-rudstone with micritized bioclasts (MF 10).
Sample DD26.3. Scale: 5 mm 8. Bio-rudstone with micritized
bioclasts (MF 10). Sample DD14.5. Scale: 5 mm
93
micritic and calcisiltic laminae in MF 3c indicates
alternating bedload and suspension transport. Micritic
intraclasts in breccia (MF 2) have been probably derived
from disrupted stromatolitic laminae, which were ex-
humed and buried again in the same type of sediment.
Mudstones (MF 1) often occur in the upper part
of shallowing upward, lagoonal-peritidal sequences and
have comparable equivalents in the Kössen Formation
(Kuss 1983; Ehses and Leinfelder 1988; Stanton and
Flügel 1989). The fenestral fabric and close association
with laminated types indicate a peritidal origin (Bystr
potok and Rztoky sections). A low diverse fauna of
agglutinated foraminifers (Glomospirella) (Gadzicki
1983) and ostracods indicates high-stress habitat in a
very shallow restricted environment, where great fluctu-
ations in salinity and temperature are probable.
Good taphonomic preservation of brachiopods in
brachiopod floatstones/packstones (MF 5) and associated
sedimentologic data (micritic matrix, absence of ooids or
intraclasts) point to an environment below the fair-
weather wave base with low-energy background condi-
tions. Complex internal structure formed by the alterna-
tion of interbeds with different packing density, various
proportions of disarticulated valves and different orien-
tations (nested or concordant) suggests episodic high-
energy influence of storm wave and currents (Aigner et al.
1978; Török 1993). The deposition of gastropod float-
stones/packstones (MF 6) probably took place in a low-
energy photic environment with a low net rate of
sedimentation and low turbidity, with good conditions
for algal growth and herbivorous gastropods. Solenopo-
racean framestones (MF 7) are characterized by preser-
vation of autochthonous small-scale algal banks, deposit-
ed in a setting below the fair-weather wave base. It is
interesting to note that benthic assemblages dominated by
solenoporaceans in the Eastern Alps (Stanton and Flügel
1987) are characterized by a different type of matrix
fabric (packstones/grainstones).
Coral framestones (MF 8) represent in-situ preserved
coral colonies. Automicritic deposits have probably been
produced by microbial processes (Kazmierczak et al.
1996). The main evidence is formed by a) gravity-defying
orientation (mucus matrix allows the accumulation), b)
differences in the comparison with the second type of
micrite (absence of other bioclasts, colour, structure) and
c) common presence in cavities. In the "Oberrhätkalk" in
the Eastern and "Calcare di Zu" in the Southern Alps,
dark homogenous microbial coatings similarly occur and
are limited mainly to the interspaces between the branch-
es of retiophyllid corals and sponges (Stanton and Flügel
1989; Lakew 1990). Comparable poorly diverse coral
assemblages dominated by high-growing Retiophyllia are
well known from the intra-platform Kössen basin and
marginal parts of the Dachstein platform (Schäfer 1979;
Piller 1981; Kuss 1983; Stanton and Flügel 1987).
According to Roniewicz & Stolarski (1999), life strategy
of epithecal phaceloid growth forms, to which Retiophyl-
lia belongs, is comparable to the mudsticker strategy
of secondary soft-bottom dwelling bivalves (Seilacher
1984). Such growth forms were well-adapted for life in an
environment with a relatively high rate of sedimentation
and turbidity. Growth forms of retiophyllid corals are
correlatable with water energy (Stanton and Flgel 1987).
In analogy to the distribution of R. clathrata A and B
morphotypes in the Eastern Alps, recognized according to
corallite diameter and robustness of colonies, branched
corals in the samples are mostly robust and closely
packed, although variation in morphotypes is high in
some cases. This can partially point to a less protected
habitat of the Retiophyllia assemblage in the Fatra
Formation with relatively higher water energy. However,
as interstices between coral branches are filled with
micrite and the proportion of sparite cement and bioclas-
tic debris is low, their habitat was probably situated below
the fair-weather wave base. Low species diversity of
patch-reef/biostrome assemblages, in contrast to some
highly diverse assemblages with corals, sponges, hydro-
zoans and tabuluzoans from the Northern Calcareous Alps
(Zankl 1969; Schäfer 1979; Dullo 1980; Wurm 1982;
Stanton and Flügel 1987, Turnek et al. 1999) or Western
North America (Stanley 1979) can be most likely related
to the short-term environmental instability of habitats in a
very shallow, intra-platform setting (Stanton and Flügel
1987). An uneven patchy distribution of coral aggrega-
tions can point to a high spatial variation in environmental
conditions or chance aspects of larval dispersion, first
recruitment and subsequent success (e.g. competition
exclusion) in survival.
Bio-floatstones with micritized corals (MF 9) are
characterized by higher alteration in comparison to coral
framestones, due to higher intensity of bioerosion/mi-
critization and episodic influence of high-energy storm
events (intraclasts, packing, thin well-sorted interlayers).
It represents a parautochthonous fossil assemblage. Pri-
mary sparitic cement is lacking, indicating primarily a
low-energy environment between the fair-weather and
normal-storm wave base.
Fabric criteria of rudstones with micritized bioclasts
(MF 10) indicate an environment above the fair-weather
wave base, with a long-term high-energy current (con-
cordant orientations) or wave activity (edgewise orienta-
tions). High degrees of taphonomic damage point to a
prolonged exposure time on the sediment/water interface
(Kidwell and Bosence 1991; Perry 1998). However,
variation in preservation and the presence of grains of
different origin (peloids, ooids, intraclasts) indicate a
complex burial/exhumation history. In some cases,
episodically storm-reworked, rapidly deposited beds can
mimic fabric pattern indicative of a long-term high-
energy environment. The biofabric of bimodally-sorted
rudstones/grainstones (MF 11) indicates that the most
important process was probably a high-energy current
event which controlled the preferred orientation of bi-
valves. High levels of taphonomic alteration were prob-
ably mainly influenced by former long-term depositional
history. Bio-grainstones (MF 12) occur in the uppermost
part of the coarsening-upward cycles, or they form
intercalations in the successions with low-energy de-
94
posits. Fabric criteria point to the deposition of small-
scale skeletal banks/shoals under long-term high-energy
conditions caused by fair-weather wave activity or fre-
quent episodic storm activity (Ball 1967; Hine et al.
1981). A high proportion of abrasion indicates influence
of wave activity and a high degree of micritization and
encrustation indicates long residence time on the sea-floor
and, therefore, reduced net rate of sedimentation (Kobluk
and Risk 1977).
The sedimentary features typical of inter- or subtidal
oolite shoals, beaches or bars such as large bed thickness
and cross-bedding (Wilson 1975; Hine 1977; Inden and
Moore 1983) are lacking in oo-grainstones (MF 13). In
the recent, aragonitic radial ooids were reported from
relatively lower-energy environments, while in the high-
est-energy conditions (the crests of bars) the crystals
become flattened and are broken into a tangential orien-
tation (Simone 1981; Gaffey 1983; Strasser 1986; Tucker
and Wright 1990). Ooids with comparable microstructure
from Purbeckian limestones originated in intermittently
agitated water (Strasser 1986). Low-Mg calcitic radial
delicate microstructure is probably primary (Kuss 1983;
Miík 1997) Although it is assumed that the "aragonite
sea" was typical of the whole Triassic (Sandberg 1983;
Hardie 1996; Stanley and Hardie 1998), the Late Triassic
is characterized by the dominance of originally calcite
ooids, in contrast to the Early and Middle Triassic
(Wilkinson et al. 1985).
In pel-packstones (MF 14), restricted diversity of
bioclasts and dominance of peloids indicate deposition in
a low-energy, perhaps peritidal, environment with poor
connection with the open basin. Intra-packstone type (MF
15) is comparable to the coated-grain facies from the
Kössen Formation (Kuss 1983), which passes laterally
into the coral biostrome and mound facies. The same
situation is also preserved in the Fatra Formation, where
this type (e.g. Dedoova, Boriov) laterally passes into the
coral limestones with autochthonous coral thickets (Re-
vfflcky Mlyn section). In general, this type has been
attributed to the "reef-detritus mud facies" by Flügel
(1981), typical of a protected reef-slope. On the basis of
the sedimentologic (well-sorted bioclastic-intraclastic
matrix, local winnowing of micrite, absence of primary
sedimentary structures) and high variation in taphonomic
alteration, it is possible to imagine an unstable exposed
shallow subtidal environment above the storm wave base
with higher rates of environmental changes (with periods
with higher water energy) leading to a complex burial/
exhumation history of particles. The particles are pre-
dominantly derived from the patch-reef/biostrome facies.
Poor sorting of ruditic shell material, variations in
taxonomic composition in the horizontal direction and
presence of large coral colonies indicate a local pa-
rautochthonous origin affected by storm activity, exclud-
ing extensive lateral transport.
The composition and preservation of components in
oobio-packstones (MF 16) indicate a complex origin,
probably related both to out-of-habitat transport and time-
averaging. Ooids can be deposited in depressions adjacent
to oolithic banks/bars or can represent residual in-situ
components when local setting changes from high- to
low-energy conditions. Subtypes with a high proportion
of components encrusted by foraminifers are mostly
typical of relatively protected back-barrier areas with
moderate water energy.
A high degree of taphonomic alteration, fabric criteria
and stratigraphic position immediately above peritidal
deposits indicate that intrabio-packstones/grainstones
(MF 17) represent a lag deposit originating under a much
reduced rate of sedimentation related to long-term win-
nowing and particle reworking.
The relatively good taphonomic preservation of bi-
valves in bivalve floatstones (MF 18), low proportion of
bioclastic debris and absence or scarcity of microintra-
clasts and ooids indicate a protected low-energy environ-
ment with poor storm reworking. Macrobenthic assem-
blages dominated by bivalves are preserved in-situ and
are comparable to those from the lower part of the Kössen
Formation (Placunopsis-Bakevellia biofacies, Golebiows-
ki 1991).
Bio-floatstones (MF 19) and bio-wackestones/pack-
stones (MF 20) with micritized bioclasts are typically
associated with an internal complex stratification, indi-
cating high-energy episodic storm-reworking and com-
plex taphonomic pathways. The two types differ basically
in the degree of sorting and packing, suggesting different
degrees of storm overprint. A high degree of micrization/
bioerosion on both external and internal surfaces suggests
a long post-mortem residence time on the sediment/water
interface. The presence of encrusted and coated, locally
also fragmented, ooids, the occurrence of similar-sized
allochems without ooidic layers, and the variable preser-
vation of co-occuring bioclasts points to their complex
origin caused by transport or by environmental conden-
sation due to rapid changes in environmental factors.
Higher water energy could have been caused by episodic
storm events or long-term fair-weather wave activity,
which led to the accumulation and sorting of al-
lochthonous material together with carbonate mud in an
adjacent depression near the subtidal skeletal banks.
Crinoid wackestones/packstones (MF 21) were deposited
in the environment around the storm wave base. Crinoid
ossicles are probably parautochthonous.
Facies associations
Facies types were subdivided according to their environ-
mental interpretation, vertical and lateral transitions into
four basic types of facies associations (facies groups
deposited in the same general environment with local
differences): 1. peritidal (or perimarine) environment, 2.
shallow subtidal environment, above fair-weather wave
base, 3. above normal storm wave base and 4. above
maximum storm wave base.
The peritidal environment includes supratidal and
intertidal flats, tidal islands and restricted depressions.
These deposits are characterized by the presence of
95
96
biolaminites, the scarcity and poor diversity of benthic
fauna, evidence of dessication or shrinkage and short-
term high-energy events. This facies association com-
prises 4 basic microfacies types: mudstones (MF 1),
breccias (MF 2), laminated bindstones (MF 3) and pel-
packstones (MF 14).
The shallow subtidal environment above the fair-
weather wave base is characterized by the presence of a
facies association showing signs of long-term water
agitation (packing, sorting, poor taphonomic preservation,
ooids). They were deposited in subtidal skeletal and
oolithic banks, incipient shoals and bars and adjacent
back-barrier depressions. 5 microfacies types involve bio-
rudstones (MF 10), bio-rudstones/grainstones (MF 11)
and grainstones with micritized bioclasts (MF 12), oo-
grainstones (MF 13) and oobio-packstones (MF 16).
An environment above the normal storm wave base
can be compared to open lagoons with normal salinity
and coral patch-reef/biostrome development, or restricted
lagoons with abnormal salinity. This facies association is
characterized by features pointing to low-energy back-
ground conditions (micritic matrix-supported fabric, rel-
atively good preservation of bioclasts) and by presence of
poorly or moderately diverse level-bottom and patch-reef
macrobenthic assemblages with bivalves, gastropods,
brachiopods, echinoderms, corals, sponges and red algae
(Fig. 15A). Typically, facies types are characterized by a
complex internal stratification on the bed scale and show
evidence of short-term high-energy overprint, which is
attributable to episodic storm events. This facies associ-
ation includes floatstones/packstones with brachiopods
(MF 5), gastropods (MF 6), floatstones with micritized
corals (MF 9), micritized bioclasts (MF 19) and wacke-
stones/packstones with micritized bioclasts (MF 20).
Below the normal storm wave base, deposits show no
evidence of substantial reworking or erosion, although
traces of storm-induced winnowing (pavements with
skeletal concentrations) or deposition from seaward
flowing storm-surge currents (thin packstone interbeds)
were preserved. Benthic assemblages are typically au-
tochthonous. Microfacies types can overlap with those
from the preceding facies association, with definitive
assignment based mostly on subtle taphonomic differ-
ences in the degree of storm-reworking (MF 4, 5, 6, 7, 8,
9, 18, and 21).
Environmental gradients
Although the DCA ordination of the exhaustive data set
(Fig. 16A) is obviously affected by data heterogeneity
(Shi 1993), a continuous variation between microfacies
types is apparent and some basic trends are visible. Along
the first dimension, the samples representing shallow
subtidal setting below the fair-weather wave base, repre-
sented by framestones and floatstones with corals (MF 8
and 9) on the right, pass into the mixture of samples with
various degrees of high-energy overprint. However,
oobio-packstones (MF 16) and oo-grainstones (MF 13)
are situated on the left and are isolated from the rest.
Therefore, the first dimension can be possibly correlated
with the long-term wave activity gradient. Ordination of
the reduced data set in the coordinate system of the first
two dimensions shows relatively distinct separation of
facies types (Fig. 16B). In this data set, including only
microfacies types with benthic assemblages unaffected by
transport or strong condensation (Fig. 15B), there is a
gradational relationship among microfacies types which
are well-defined and mostly non-overlapping. The first
dimension can perhaps be related to a gradient in the
substrate stability/water turbidity, with coral thickets
living in a generally muddy environment (cf. Roniewicz
and Stolarski 1999). Although the interpretation of the
second axis in DCA is less clear (Kenkel and Orloci
1986), along the second dimension, there is a continuous
gradation from poorly diverse bivalve- and gastropod-
dominated microfacies with rare euhaline taxa in the
lower part, to facies types with red algae, echinoderms,
corals in the middle part, and brachiopod floatstones (MF
5) in the upper part of the plot. This dimension may
reflect a salinity gradient.
Based on the correlation of the individual sections
(Tomaovch 2002, see above), there are three relatively
well-defined unconformities, subdividing the stratigraphic
column of the Fatra Formation in four large-scale
depositional sequences (see description of sections above,
Fig. 4, 7­10). Although an interpretation of the sequence
stratigraphy is beyond the scope of this paper, in order to
interpret and understand spatial facies relationships, a
preliminary assessment of their temporal distribution
patterns is discussed here. Within the depositional se-
quences that are defined according to these unconformi-
ties, vertical distribution of facies associations show a
characteristic repetitive pattern. Therefore, in a simplified
scheme, the distribution of microfacies types/facies asso-
ciations in the lowermost large-scale sequence (Fig. 15B)
of the Fatra Formation is used as the reference for
reconstruction of the depositional environment (Fig. 17)
here. Vertical changes in facies types enable us to
interpret lateral shifts in the depositional environment
(Walther`s Law). It is important to note that this recon-
struction does not include the complicated bottom topo-
graphy, but is primarily focused on lateral relationship of
facies types (Fig. 17).
1. In the lower part of the large-scale depositional
sequence, MF types 18 (bivalve floatstones), 19 (bio-
floatstones with micritized bioclasts) and 20 (bio-
packstones/wackestones with micritized bioclasts) al-
ternate with grainstones and bivalve rudstones (MF 10-
Fig. 15 A Spatial variation in the facies development of coral
patch-reef/biostrome facies in Dedoova ­ Frèkov. The distance
between A and E section is 30 m. B. The correlation of the first
large-scale sequence with coral patch-reef/biostrome facies (lower
part of the Fatra Formation). The distance between Rztoky-
Nolèovo (NW part) and Sviniarka-Mal Zvolen (SE part) is about
25 km
97
12), often forming shallowing-upward lagoonal-skele-
tal bank sequences. One of the most typical features is
the presence of small-scale structures related to storm-
reworking in MF 19 and 20, which are therefore
usually characterized by a complex small-scale strati-
graphic architecture. Although DCA based on compo-
nent frequencies in microfacies types revealed an
environmental gradient related to wave/water energy,
incorporation of fabric/geometric and taphonomic
criteria allows recognizing a depth-related environ-
mental gradient with higher confidence (Fig. 17A).
Areas lying above the fair-weather wave base subject-
ed to long-term high-energy influence or multiple
storm events are characterised by the presence of well-
sorted bio-grainstones, oo-grainstones and bivalve
rudstones, commonly with amalgamation. Below
the fair-weather wave base, simple or multiple-event
storm-reworked deposits occur, with a bivalve-domi-
nated assemblage. Variation in the degree of bioero-
sion/micritization points to the complex history related
to the rate of burial/residence time on the sea-floor.
Towards the more protected environment below nor-
mal storm wave base, intensity of storm event de-
creases and relatively undisturbed bivalve floatstones
are preserved. In depressions lying in adjacent posi-
tions to high-energy ooid-skeletal banks, oobio-pack-
stones were deposited. In landward direction, low-
energy peritidal flats have been formed. In summary,
Fig. 16 A Detrended corre-
spondence analysis of all sam-
ples showing ordination of
samples and components using
dimensions 1 and 2. B. De-
trended correspondence analy-
sis of reduced data matrix
showing ordination of samples
and bioclasts using dimensions
1 and 2. Numbered points re-
present individual samples. Ex-
planations: Biv--bivalves,
Gpd--gastropods, Bpd--bra-
chiopods, Ech--echinoderms,
Ost--ostracods, Cor--corals,
Spo--calcareous sponges,
For--foraminifers, Ssf--sessile
foraminifers, Ral ­ red algae,
Gal ­ green algae, Oo ­ ooids,
Int ­ intraclasts, Pel ­ peloids
98
this stage can be termed as a shallow lagoon with tidal
flats and skeletal banks and poorly diverse bivalve-
dominated assemblages.
2. In the middle part of the large-scale sequence, float-
stones, packstones and framestones with poorly or
moderately diverse macrobenthic assemblages (MF 5,
7, 8, 9) are dominant. Coral assemblages are repre-
sented by dm-scale biostromes or by small-scale, 2-m
thick patch-reefs composed of several stacked coral
colony aggregations (Fig. 15A, Fig. 5). The dominance
of a matrix-supported fabric and the presence of
stenohaline taxa indicate the deposition in an open
Fig. 17 Schematic reconstruction of lateral facies relationship in an
environmental gradient in three different stages, developed within
one large-scale sequence. A. Shallow lagoon with tidal flats/
skeletal banks and poorly diverse bivalve-dominated assemblages
B. Deeper lagoon below FWWB with euhaline assemblages C.
Restricted peritidal environment
99
lagoon below the fair-weather wave base (Fig. 17B).
The horizontal dimension of 1 to 2-m-thick coral
patch-reef/biostrome between Dedoova-Frèkov and
Mal Zvolen-Sviniarka attains about 10 km (Fig. 15B).
In the marginal, NW part, high-energy skeletal banks
were deposited. The evidence of storm-reworking
points to a relatively shallow environment above
normal storm wave base. Most exposed habitats are
represented by bio-wackestones/packstones with mi-
critized bioclasts (MF 20) and bio-floatstones with
micritized corals (MF 9). In areas characterized by
lower intensity of storm activity and/or lower inten-
sity of taphonomic alteration, undisturbed brachiopod
floatstones and monotypic coral aggregations (Retio-
phyllia framestones) were preserved. This stage is
termed as a deeper lagoon below FWWB with benthic
assemblages dominated by stenohaline taxa.
Patch-reef and biostrome-like areas played several
roles in the carbonate production. They trapped and/or
stabilized mostly fine-grained sediments, formed the
sites of automicrite precipitation, and hosted a rela-
tively diverse spectrum of carbonate-secreting organ-
isms. On the one hand, taphonomic processes leading
to precipitation of automicritic crusts probably stabi-
lized and enhanced preservation potential of coral
colonies. The presence of automicrite and encrusta-
tions (foraminifers) in intra-skeletal coral cavities
indicates their post-mortem origin. On the other hand,
corals are commonly preserved in parautochthon-
ous deposits (MF 9) with signs of storm reworking
(Fig. 175) and substantial bioerosion. It is not easy to
distinguish between these two interrelated destruction-
al factors and evaluate which was more important in
destroying coral thickets. In some beds, there is
evidence of extensive degradation of in-situ corals by
bivalve macroborings (Fig. 51, Fig. 66). There is a
positive correlation between the intensity of bioerosion
and the degree of fragmentation of corals. In frame-
stones (MF 8) with a low proportion of fragmented
corals, the intensity of bioerosion is low in contrast to
bio-floatstones with micritized corals (MF 9). It is
possible that the higher activity of bioeroders related to
local fluctuations in nutrient supply or turbidity made
corals more susceptible to the destruction by storm
activity (Hallock and Schlager 1986; Hallock 1988;
Perry 1999). This can be confirmed by the fact that the
regeneration potential of epithecate corals (Roniewicz
and Stolarski 1999) is relatively low due to a lack of an
edge-zone (tissue covering the external surface and
repairing injuries).
3. In the upper part of the large-scale sequence, imme-
diately below the terminal unconformity, mudstones
and stromatolitic mudstones are dominant among
various facies types (Fig. 15B). At this time, over
most of the area, mudstones, laminated mudstones and
mudstones with poorly diverse microfauna (ostracods,
foraminifers) prevailed (Fig. 17C). However, it has
been established that typical peritidal features (e.g.
fenestrae, desiccation, evaporates) can also develop in
non-tidally influenced environments, e.g. fluctuations
in sea level may be caused by wind activity or
seepages in back-barrier lagoons (Tucker and Wright
1990).
Depositional environment
The spatial arrangement of facies types along the depth-
related environmental gradients points to the importance
of water energy as one of the main control factors
influencing their distribution patterns. Long-term wave
energy and possibly tidal currents influenced sediment
composition and fabric in skeletal and oolithic banks
above the fair-weather wave base. However, the absence
of large-scale barrier-bank complexes and small thick-
nesses are indicative of a relatively shallow depth level of
the FWWB. During episodic storm events, in addition of
substantial overprint of shoreface setting, areas below the
fair-weather wave base were influenced by erosion, rapid
burial and redeposition of sediment by storm waves and
currents. The main biologic carbonate production took
place below the fair-weather wave base, where coral
patch-reef/biostrome assemblages and level-bottom bent-
hic assemblages were living. The distribution of macro-
benthic taxa can be correlated similarly with depth in a
simplified scheme. This pattern is visible in the ordination
of samples and taxa in the DCA, where trends related to
water energy level, substrate stability and salinity can be
inferred. This view about the position of coral-patch reefs
differs from that in the depositional model of Michalik
(1982), where coral patch-reefs are situated in the area of
main wave activity. However, phaceloid growth mor-
phology, sedimentologic (mud baffling, structures indi-
cating storm activity) and taphonomic data (preservation
state) are indicative that low-energy conditions in the
vicinity of the storm wave base were their main preferred
habitat.
On this spatial scale of analysis, facies patterns are
therefore typical of ramp morphologies, where energy
gradients are a consequence of gradual depth changes and
higher production is limited to low-energy setting below
FWWB in mid-ramp position (Burchette and Wright
1992). This can be a consequence of several factors
related to the dominance of destructive taphonomic
processes (high rate of degradation due to bioerosion
and storm activity, e.g. Kuss 1983; Bernecker et al. 1999),
perhaps the ecology of frame-building organisms (ac-
cording to Stanton and Flügel 1987, branching retiophyl-
lid corals mostly did not build rigid wave-resistant
framework that could withstand the highest wave activity,
but there are contradictory opinions, see Piller 1981;
Schäfer 1984; Schäfer and Senowbari-Daryan 1981),
environmental restriction/instability of Fatric intra-shelf
setting leading to poor species richness (Michalík 1982),
and/or slow subsidence or slow eustatic sea level rise
(limited accommodation space). A comparable deposi-
tional model was developed for the lower part of the
Kössen Formation (Kuss 1983). However, due to the
100
increase of the accommodation potential with relative sea
level rise in the Upper Rhaetian, large-scale patch-reefs
developed at distally-steepened ramps at the Kössen
Basin margin or formed isolated structures within the
Kössen Basin (Stanton and Flügel 1995). This is in
contrast to the Fatric Unit, where the thickness of coral
patch-reefs/biostromes attains maximally 4­5 m.
Given the abundant evidence of storm-reworking in
the Fatra Formation, this intra-platform setting can be
interpreted as storm-dominated. Although a typical tem-
pestitic succession (Aigner 1982, 1985), including hori-
zontal, hummocky-cross and ripple stratification, is most-
ly not preserved, several consistent features, such as
erosional boundaries and grading associated with micritic
fabric are indicative of storm origin. The evaluation of
tidal activity is problematic and remains inconclusive at
this point. Due to well-known low preservation potential
of inter-supratidal deposits in modern seas, the absence
of some typical tidal structures (e.g. herringbone cross-
stratification) cannot be directly taken at face value. In
a traditional model, the depositional setting of shallow
epeiric seas is supposed to be essentially tideless due to
bottom friction dampening tidal range. However, Pratt
and James (1986) developed a model of a tide-dominated
carbonate platform, based on assumptions that tidal height
increases with increasing continental shelf area (Klein and
Ryer 1978; Cram 1979); bottom friction is important only
if there is substantial turbulence in the bottom layer and
tidal currents themselves directly create the sea-floor
topography.
In general, high variation in distribution of shallow
water facies types and paleogeographic data (relatively
restricted intra-shelf position) indicate that environmental
conditions in respect to water energy, salinity or water
turbidity were relatively unstable and ecologically re-
stricted. This is supported by low or moderate diversity of
both level-bottom and patch-reef/biostrome assemblages
in comparison to those in the Eastern Alps (Golebiowski
1991) or dominance of eurytopic taxa (Michalík 1979,
1982).
Conclusions
21 microfacies types of the Rhaetian Fatra Formation
supported by a cluster analysis represent a storm-domi-
nated shallow environment. Main components are bi-
valves, gastropods, brachiopods, echinoderms, corals,
foraminifers and red algae, ooids, intraclasts and peloids.
The typical feature is the considerable lateral facies
variation. Thus the depositional environment consisted of
a wide spectrum of facies types, from peritidal flats/
islands with algal or microbial mats, skeletal and oolitic
banks and bars, open or restricted lagoons to small-scale
coral biostromes and patch-reefs. Along the depth-related
environmental gradient primarily linked to water energy,
they form 4 facies associations corresponding to a peri-
tidal setting, high-energy shoreface (above fair-weather
wave base), shallow subtidal setting above normal storm
wave base and shallow subtidal setting above maximum
storm wave base.
The distribution and preservation of components were
mainly influenced by the position of base level (FWWB),
storm activity and differences in rate of biogenic carbon-
ate production between individual settings. Water depths
obviously remained very shallow throughout the deposi-
tion of the Fatra Formation. The main site of coral patch-
reef/biostrome carbonate production was situated below
the fair-weather wave base. Poorly diverse Retiophyllia-
dominated coral assemblages form locally autochthonous
several dm-thick colony aggregations or more commonly
parautochthonous assemblages with evidence of the
storm-reworking and substantial bioerosion by boring
bivalves and microborings. Ordination methods indicate
that changes in water energy, substrate stability/turbidity
and salinity had substantial effects on the distribution of
benthic groups.
The reconstruction of the depositional environment
involves three stages, differing in the position of relative
sea level, namely a) shallow lagoon with tidal flats/
skeletal banks and poorly diverse bivalve-dominated
assemblages, b) deeper lagoon below FWWB with
euhaline level-bottom and patch-reef/biostrome assem-
blages and c) restricted peritidal environment.
Facies types and assemblages are closely comparable
to those known from the uppermost Triassic of the
Eastern and Southern Alps (Hochalm Member of the
Kössen Formation or Calcare di Zu Formation), pointing
to similar intra-shelf depositional conditions. The absence
of large-scale patch-reefs and the poor diversity of level-
bottom and patch-reef/biostrome assemblages indicate the
Fatric intra-platform setting was more restricted from the
open ocean than intra-shelf habitats in the Eastern or
Southern Alps at the end of the Triassic.
Acknowledgements This project had started at the Department of
Geology and Paleontology of the Comenius University (Bratislava)
and Geological Institute of Slovak Academy of Sciences (Bratisla-
va). I am very indebted to J. Michalík and R. Aubrecht for their
supervising. I thank also M. Miík, M. Kovè, M. Rakffls, J. Schlögl
(Bratislava), J. Sotk, A. Bendík (Bansk Bystrica) and J. Farka
(Ottawa) for their help and encouragement. I am indebted to W.
Kiessling (Berlin) and W. Piller (Graz) for critical reviews. I thank
F. T. Fürsich and M. Wilmsen (Würzburg) for discussions and
critical comments on the manuscript and E. Roniewicz (Warszawa)
for help with determination of corals. This study has been funded
by the AAPG Grant in Aid 2001 and is a contribution to the IGCP
Project 458 - Triassic-Jurassic boundary events.
Appendix
The appendix consists of Fig. 18.
101
102
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