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GEOLOGICA CARPATHICA, OCTOBER 2009, 60, 5, 351—379 doi: 10.2478/v10096-009-0027-y
Lithofacies and age data of Jurassic foreslope and basin
sediments of Rudabánya Hills (NE Hungary) and their
tectonic interpretation
SZILVIA KÖVÉR
1
, JÁNOS HAAS
1
, PÉTER OZSVÁRT
2
, ÁGNES GÖRÖG
3
, ANNETTE E. GÖTZ
4
and SÁNDOR JÓZSA
5
1
Geological, Geophysical and Space Science Research Group of the Hungarian Academy of Sciences, Pázmány Péter str. 1/C,
H-1117 Budapest, Hungary; koversz@yahoo.com; haas@ludens.elte.hu
2
Hungarian Academy of Sciences – Hungarian Natural History Museum, Research Group for Paleontology, P.O. Box 137,
H-1431 Budapest, Hungary
3
Eötvös University, Department of Paleontology, Pázmány Péter str. 1/C, H-1117 Budapest, Hungary
4
Institut für Angewandte Geowissenschaften, Technische Universität Darmstadt, Schnittspahnstraße 9, D-64287 Darmstadt, Germany
5
Eötvös University, Department of Petrology and Geochemistry, Pázmány Péter str. 1/C, H-1117 Budapest, Hungary
(Manuscript received April 7, 2008; accepted in revised form March 26, 2009)
Abstract: Jurassic sedimentary rocks of the Telekesvölgy Complex (Bódva Series), Telekesoldal Complex (Telekesoldal
Nappe) and the Csipkés Hill olistostrome in Rudabánya Hills (NE Hungary) were sampled for microfacies studies and
interpretation of the depositional environments. The Telekesvölgy Complex is made up of reddish to greenish marl, oc-
casionally containing limestone olistoliths – gradually progresses from the Norian Hallstatt Limestone of the Bódva
Series – then grey marl, which may correspond to the latest Triassic Zlambach Formation. This variegated marl progresses
into grey marl and calcareous marl, containing crinoid fragments. It may be interpreted as a hemipelagic facies, relatively
close to submarine highs. Bajocian to Lower Bathonian black shales, rich in radiolarians and sponge spicules representing
typical deep pelagic facies, are also assigned to the Telekesvölgy Complex. The Telekesoldal Complex represents a mélange-
like subduction-related complex that consists of black shales, sandstone turbidites and olistostrome beds, and deposited by
gravity mass flows. A relatively deep marine basin in the proximity of a submarine slope is likely to be the depositional
environment of this unit. The clasts of the olistostromes are predominantly Middle to Upper Triassic pelagic limestones,
rhyolite and basalt. Subduction related nappe stacking of the ocean margin during the Middle to Late Jurassic may have
created suitable conditions for this sedimentation pattern. Bajocian—Callovian age of the complex was proved by the
revision of the radiolarian fauna and new palynological data, the first from the Jurassic of the Aggtelek-Rudabánya Hills.
The Csipkés Hill olistostrome consists of carbonate turbidite beds containing Jurassic platform derived foraminiferal and
olistostrome horizons with Middle—Upper Triassic limestone clasts of red Hallstatt facies.
Key words: Jurassic, Neotethys, subduction-related complex, mass-flows, microfacies, Foraminifera, Radiolaria,
palynomorphs.
Introduction
The last geological mapping project in the early eighties re-
sulted in a new geological and tectonic map of the Aggtelek-
Rudabánya Hills (Less et al. 1988; Szentpétery & Less
2006). Recognition of nappes can be considered the most
important result of this project. However, the definition and
accordingly the number of the structural units, the superposi-
tion of the nappes, the sedimentary features and ages of the
sequences have not been clarified. The previous investiga-
tors pointed out, that there are metamorphic and non-meta-
morphic structural units forming a complex nappe stack
(Grill et al. 1984; Árkai & Kovács 1986; Less et al. 1988;
Less 2000; Szentpétery & Less 2006). According to their
concept, this nappe stack is composed of three main tectonic
units, and characterized by different kind of rocks and sub-
jected to different degrees of metamorphism.
In the last years a new project should obtain new structural
and metamorphic data for a better understanding of the struc-
tural position, the deformation history and the metamorphic
conditions of the nappes of Aggtelek-Rudabánya Hills (Fodor
& Koroknai 2000, 2003; Kövér et al. 2005, 2006, 2007).
In the course of these investigations new stratigraphical
and sedimentological questions came up concerning the Ju-
rassic sequences. These sequences have been studied since
the middle of the 19th century (Foetterle 1869). Until the
1980-ies the whole Mesozoic succession was assigned to the
Triassic. As a result of the works of Grill & Kozur (1986),
Grill (1988) and (Dosztály 1994) the Jurassic age of these for-
mations became generally accepted about 20 years ago. How-
ever, our knowledge of the structural position, depositional
environment and exact age of the Jurassic formations, their re-
lations with the underlying Triassic basement, and the correct
order of the formations has not been clarified, until now.
On the basis of lithological and paleontological data, the pre-
vious researchers subdivided the uppermost Triassic-Jurassic
sequences into two lithostratigraphic units: the Telekesvölgy
Complex (TVC) and Telekesoldal Complex (TC) although the
same units were also referred as formations and groups, respec-
tively (Grill & Kozur 1986; Grill 1988; Dosztály 1994; Dosztá-
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KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
Fig. 1. Location of the study area with simplified structural elements (after Kövér et al. 2008), geographical names and locations of the
boreholes. Line A—B indicates the course of the cross-section (Fig. 2).
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LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
ly et al. 1998). Grill (1988) subdivided the TVC into three sub-
units: a) variegated (reddish-greenish) claymarl sequence of
Late Triassic age. It was regarded by Dosztály et al. (1998) as
an atypical development of the latest Triassic Zlambach Marl
on the basis of lithological comparison; b) a siliceous crinoidal
limestone and marl unit that was called “spotty marl” by Dosz-
tály et al. (1998); and c) black claystone. Grill (1988) subdivid-
ed the TC into the following lithofacies types: a) siliceous marl
unit; b) rhyolite; c) shale with sandstone olistoliths and d) shale
with conglomerate and limestone olistoliths. Slightly modifying
this subdivision, Dosztály et al. (1998) distinguished two units:
a) grey claystone—siliceous marl with subvolcanic rhyolite bod-
ies and b) olistostromal unit containing a sandstone olistolithic
and a limestone-rhyolite olistostrome interval.
The Jurassic parts of both complexes were interpreted as
the products of slope and basin environments, most likely in
a Jurassic back arc basin (Grill 1988).
Geological mapping revealed some other occurrences,
which are supposed to be uppermost Triassic or Jurassic as
well, and could not be classed among the previously men-
tioned complexes.
1. Olistostrome at Hidvégardó contains redeposited clasts
of a whole Bódva-type (“Hallstatt facies”) Anisian-Norian
sequence: early Middle Triassic grey platform carbonates
(Steinalm Formation), Middle and Upper Triassic red cherty
limestones (Bódvalenke Formation), and Upper Triassic
pink and grey limestones (Hallstatt Formation) (Szentpétery
& Less 2006).
2. A small, previously unmentioned sequence was recently
encountered on the southeastern slope of Csipkés Hill
(Fig. 1b) (Csipkés Hill was also called Bizó-tető Hill in some
references) (Kövér 2005). It consists of alternating beds of car-
bonate turbidites and silicified marls that are overlain by fine-
grained, and followed by coarse-grained olistostrome beds.
These uppermost Triassic(?)—Middle Jurassic formations
have a great importance for understanding the Jurassic evolu-
tion of the Neotethys Ocean. However, no detailed report on
the sedimentological characteristics and component analysis of
the redeposited clasts has been published so far (except from the
Szalonna-Perkupa road cut key section of TC (Kovács 1988)).
The aim of the present paper is to define lithofacies units,
to summarize the facies characteristics of the defined units,
to provide interpretation for the provenance of the redeposit-
ed clasts and depositional environments, and last but not at
least to revise the existing radiolarian data, and provide new
age data by foraminiferal and palynomorph investigations.
Fig. 2. Cross-section of the area after Kövér et al. (2008).
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KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
Geologic setting
The Rudabánya Hills are located in NE Hungary (Fig. 1a),
and built up by a nappe stack of Upper Permian—Middle Juras-
sic sediments. They are located within the Cretaceous—Tertia-
ry Darnó Fault Zone bounded by major faults to the NW and
SE (Fig. 1c). The Darnó Zone is an important NNE-SSW
structural element, located in NE Hungary reaching the
southernmost part of the Slovak Republic. Earlier works
considered both boundary faults as a Miocene sinistral struc-
ture (Less & Szentpétery 2006; Szentpétery 1997), but the
newest review of Fodor et al. (2005) – on the basis of fault
slip data – challenged this hypothesis. They pointed out,
that the Darnó Line does not represent a first-order nappe/
terrain boundary during the Late Jurassic-Cretaceous orogeny.
The northwestern segment of this fault zone is actually the
boundary between the Aggtelek Hills containing only Upper
Permian and Triassic formations and the Rudabánya Hills
containing uncertain Paleozoic rocks (Less et al. 1988), and
Upper Permian—Middle Jurassic formations (Less et al. 1988).
Jurassic rocks occur in two structural units. The Upper Trias-
sic(?)—Middle Jurassic Telekesvölgy Complex is part of the
Bódva Unit (Kövér et al. 2006, 2007, 2008), which is made up
of Upper Permian to Middle Jurassic formations (Figs. 1a, 2).
The Telekesoldal Complex represents an individual nappe
(Figs. 1a, 2) overlaying the Bódva Nappe (Kövér et al. 2006,
2007, 2008). The TC was subject to ductile deformation in
three phases and a higher anchizonal—lower epizonal meta-
morphism during the Cretaceous (Árkai & Kovács 1986;
Kövér et al. 2007). From the sedimentary rocks, the only
available age was Bajocian by means of the radiolarian fauna
of the lowermost shale-marl member (Grill & Kozur 1986;
Dosztály 1994).
Successions
Telekesvölgy Complex
On the basis of macroscopic observations and microfacies
studies performed on cores Rudabánya Rb-658, Szalonna
Sza-5, Szendrő Szet-4, Varbóc Va-2 cores (Fig. 1b,c), trenches
in the Telekes Valley (Tributary Valley 7 and 8) and outcrops
on Csipkés Hill (Fig. 1c) various lithofacies units could be dis-
tinguished. However, continuous sections exposing the whole
formation are not available, the relevant biostratigraphic data
are very limited and the stratigraphic superposition of the litho-
facies units is ambiguous. Figure 3 shows the most probable
lithofacies succession referring to the relevant cores and sur-
face exposures and the discussion below follows this pattern.
Variegated and grey marl
Szalonna Sza-5 core.
In Szalonna Sza-5 core Upper Triassic
red, locally cherty limestones (Hallstatt Limestone) are concor-
dantly overlain by red, green and grey marl 23 m in thickness,
that was assigned to the Zlambach Formation (Szentpétery &
Less 2006). It is followed by grey marl with slump structures in a
thickness of 30 m.
Perkupa P-74 core.
In Perkupa P-74 core, brown to grey
marls occur above the Hallstatt Formation with tectonic con-
tact and the marls are tectonically overlain by Upper Triassic
hemipelagic carbonates. This ~ 30 m thick interval may also
be assigned to the Zlambach Formation. Texture of these
rocks is rather unspecific; mudstone—wackestone containing
small bioclasts, silt-sized quartz and in one thin section poor-
ly preserved foraminifers, ostracodes, fragments of bivalves,
echinoderms and radiolarian moulds (Fig. 4). From this thin
section the following foraminiferal taxa could be deter-
mined: Aulotortus friedli (Kristan-Tollmann), A. parallelus
(Kristan-Tollmann), Semiinvoluta clari Kristan, Turrispirill-
ina minima Pantić, Lamelliconus sp., Meandrospira sp.,
Frondicularia sp., Lingulina sp. The dominance of the Invo-
lutinidae (Aulotortus, Semiinvoluta, Lamelliconus) and Spir-
Fig. 3. Simplified reconstructed stratigraphic column of the Tele-
kesvölgy Complex. The positions of the age data, the studied bore-
holes and outcrops are approximately indicated.
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LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Fig. 4. Thin section of core P-74, 170.9—171 m interval, showing wacke-
stone texture with foraminifers and fragments of bivalves. The fora-
minifer indicated by a white arrow is enlarged on the smaller photo.
illinidae (Turrispirillina) indicate a warm, well-ventillated,
shallow-water environment, like the habitat for these forms.
The co-occurence of these genera is characteristic in the
Late Triassic. Except A. friedli (Kristan-Tollmann) – which
appeared already in the lowermost Carnian – all species de-
termined only in the Norian—Rhaetian (Kristan 1957; Kristan-
Tollmann 1962, 1964; Zaninetti 1976; Salaj et al. 1983, 1988;
Trifonova 1993). According to Salaj et al. (1983), the age
range of the species T. minima Pantić is Norian-Rhaetian, al-
though it was mostly reported from the Norian (e.g. Oravecz-
Scheffer 1987).
Telekes Valley, Tributary Valley 8 section
. Brownish grey
marl, alternating with grey calcareous marl and greenish grey
shale exposed in the Telekes Valley, Tributary Valley 8 sec-
tion may also belong to this lithofacies unit but it is poorly
constrained. It contains pink limestone olistoliths which yield-
ed Late Norian conodonts (Balogh & Kovács 1977).
Csipkés Hill section 1.
In the sample taken form the Csip-
kés Hill section 1, alternating red and yellow laminae are
visible. The yellow layers consist of fine sand to silt-sized
clasts that might be silicified carbonate particles while the
red layers are radiolarian wackestones. Metre-sized lime-
stone olistoliths containing Middle Triassic Foraminifera
(det.: Bérczi-Makk) were reported by Grill (1988) from
Csipkés Hill sections 1 and 2.
Rudabánya Rb-658 core.
In Rudabánya Rb-658 core
(Fig. 5), red and green claystones alternating with grey marls
and calcareous marls were encountered above Hallstatt-type
(Kovács in Szentpétery I. & Less Gy. (Eds.) 2006) red, local-
ly cherty limestones with tectonic contact between them.
The lowermost, about 13 m thick part of this succession is
made up of red and green claystone intercalating with grey
marl. The texture of the samples studied is strongly sheared,
and altered. However, the original radiolarian wackestone
texture could be recognized (Fig. 6.1). Calcite moulds of ra-
diolarians are usually deformed showing lenticular shape.
Sponge spicules and other bioclasts can also be recognized
in a few cases. The rocks were commonly affected by dolo-
mitization and subsequent selective silicification. Under a
Fig. 5. Lithological and stratigraphic features of the Rudabánya
Rb—658 borehole with new interpretations (Kövér et al. 2008).
microscope the texture is seemingly silty shale containing dis-
seminated silt-sized quartz. However, in a lot of cases the
quartz occurs in biomoulds (Fig. 6.2) or substitutes rhombic
dolomite crystals. Accordingly, the majority of the quartz par-
ticles are probably not terrigenous grains but they formed by
diagenetic alteration and structural deformation processes.
Going upwards in the section, the proportion of the grey
marl and calcareous marl increases, while the ratio of red and
green claystone interlayers decreases. In this ~ 20 m thick
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KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
interval fine to medium sand-sized crinoid ossicles are com-
mon in a micritic—microsparitic matrix and thin crinoidal
packstone to grainstone interlayers also occur (Fig. 6.3—4).
The matrix is often, crinoids are rarely silicified. Grey siliceous
crinoidal marls and limestones akin to those in Rb-658 core
(104—122 m) were reported by Grill (1988) from the Telekes
Valley Tributary Valley 7 section and Csipkés Hill section 1.
The next ~ 20 m thick segment is made up of green and
pinkish marl and calcareous marl progressing upward into
grey marl; with the calcareous marl having a uniformly bar-
ren mudstone texture.
It is tectonically overlain by dark grey limestone, showing
microsparitic texture with no sign of any diagnostic micro-
structure or fossil, which can refer either to the depositional
environment or to the age of sedimentation. On basis of its
macroscopic features, this limestone was assigned to the
Gutenstein Formation (G. Less. pers. com).
Black siliceous shale
Varbóc Va-2 borehole.
In Varbóc Va-2 borehole the Nori-
an Hallstatt Limestone is tectonically overlain by black shale
about 80 m thick. The locally silicified shale contains large
amounts of radiolarians and sponge spicules.
Telekes Tributary Valley 7 and 8 sections.
In the western
part of the section exposed on the top of valley side of Tele-
kes Tributary Valley 8, beside a steeply dipping Upper Tri-
assic succession, black shale and siliceous shale were found.
Radiolarian wackestone, radiolarian-sponge spicule wacke-
stone and packstone (Fig. 7.1,3), sponge spicule packstone
(Fig. 7.4), and radiolarite are typical textures of this lithofa-
cies unit. In some samples sharp, erosional boundaries are
visible between the radiolarian shale and the crinoidal cal-
carenite layer (Fig. 7.5,6), the latter is formed via turbiditic
redeposition. The same texture types were found in the sam-
ples taken from black shale in the Telekes Valley Tributary
Valley 7 section.
Revision of the radiolarian fauna in Telekesvölgy Complex
The first studies of radiolarians of the Rudabánya Hills, NE
Hungary were conducted by Grill & Kozur (1986). Their
samples were collected from the Varbóc-2 borehole and from
several different outcrops in the Rudabánya Hills (i.e. Csehi-
Fig. 6. 1 – Radiolarian rich layer in radiolarian marl. Rb-658, 119.9 m. 2 – Quartz substitutes rhombic dolomite crystals or occurs in
biomoulds. Rb-658, 126 m (bottom left and right), 131 m (top). (Bottom right and top crossed polars). 3 – Fine-grained crinoidal wacke-
stone. Rb-658, 104.6 m. 4 – Medium-grained crinoidal wackestone. Rb-658, 86.7 m.
357
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
hegy, Telekes Valley—Tributary Valley 7 and 8). Radiolarians
were always found in the sequence of monotonous black to
dark grey shales, mudstones, siliceous shales, manganese
shales and dark shales (Grill & Kozur 1986). Previous bios-
tratigraphic data of radiolarian investigation presumed Aalen-
ian to the middle Bajocian ages in different sequences studied
Fig. 7. 1, 3 – Radiolarian-sponge spicule packstone, Telekes Valley. 2, 4—6 – Details of a calciturbidite layer, Telekes Valley: above an
uneven erosion surface a mudstone layer is overlain by coarse-grained crinoidal packstone that is the basal part of a carbonate turbidite
(5, 6). Sponge spicula and crinoid packstone in the higher part of the turbidite layer (4). The topmost part of the turbidite layer showing
gradual transition to pelagites of wackestone—mudstone texture (2).
in the Rudabánya Hills. According to the re-assessment of the
Varbóc-2 borehole (Dosztály 1994), the biostratigraphic age
assigned the lower part to the Aalenian, and the upper part to
the Bajocian or Bathonian. Our latest re-assessment of the ra-
diolarian biozonation of the studied samples in the Rudabánya
Hills is based on the Unitary Association Zones (UAZ95) pro-
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KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
posed by Baumgartner et al. (1995). The occurrence and the
stratigraphical distribution of the radiolarians in the examined
samples are shown in Table 1.
Varbóc-2 borehole.
The Varbóc-2 borehole penetrated the
87 m thick Jurassic monotonous black to dark grey shales,
with thin siliceous shales and cherts, and crinoidal lime-
stones intercalated with grey marl and mudstone. The 16
samples yielded abundant and moderately well preserved ra-
diolarian assemblages.
Base of the borehole: samples come from 80.9 m, 79.1 m,
77.6 m, 73.9 m, 73.0 m and from 69.7 m. The following strati-
graphically important radiolarian taxa were identified from
these samples (Figs. 8, 9): Hsuum mirabundum Pessagno &
Whalen, H. belliatulum Pessagno & Whalen, H. matsuokai
(Isozaki & Matsuda), Transhsuum maxwelli (Pessagno),
Parahsuum officerense Pessagno & Whalen, P. snowshoense
(Pessagno & Whalen), Semihsuum inexploratum (Blome),
Pseudodictyomitrella spinosa Grill & Kozur, Archaeodictyo-
mitra rigida Pessagno, Laxtorum(?) hichisoense Isozaki &
Matsuda, Canoptum hungaricum Grill & Kozur, Tetratrabs
zealis (Ožvoldová). The co-occurrence of H. mirabundum
Pessagno & Whalen (UAZ 3—6), L.(?) hichisoense Isozaki &
Matsuda (UAZ 1—4) and T. zealis (Ožvoldová) (UAZ 4—13)
indicates the UAZ 4 (Late Bajocian). However, presence of H.
belliatulum Pessagno & Whalen and H. snowshoense (Pessag-
no & Whalen) is presumable the lower part of middle Bajocian
age for this sequence as well, because these taxa co-occur in
that close range in North America (Pessagno & Whalen 1982).
Samples from 64.1 m to 3.4 m yielded the following strati-
graphically important radiolarian taxa (Figs. 8, 9): Hsuum
mirabundum Pessagno & Whalen, H. rosebudense Pessagno &
Whalen, H. matsuokai Isozaki & Matsuda, Parahsuum stanley-
ense (Pessagno), Transhsuum hisuikyoense (Isozaki & Matsu-
da), T. maxwelli (Pessagno), Semihsuum inexploratum (Blome),
Pseudocyrtis buekkensis Grill & Kozur, Eucyrtidiellum no-
dosum Wakita, Eucyrtidellum cf. E. unumaense (Yao), Sti-
chocapsa robusta Matsuoka, Stichocapsa sp. E. Baumgartner,
Archaeodictyomitra rigida Pessagno, A. exigua Blome, A. cel-
lulata O’Dogherty, Goričan & Dumitrica, A. prisca Kozur &
Mostler, Pseudodictyomitrella hexagonata (Heitzer), Protunu-
ma turbo Matsuoka, Canoptum hungaricum Grill & Kozur,
Dictyomitrella (?) kamoensis Mizutani & Kido. The co-occur-
rence of H. mirabundum Pessagno & Whalen (UAZ 3—6) and
Stichocapsa robusta Matsuoka (UAZ 5—7) indicates the UAZ
5—6 (latest Bajocian to Early Bathonian), furthermore the pres-
ence of Stichocapsa sp. E. Baumgartner (UAZ 5) presumably
indicates the UAZ 5 (latest Bajocian to Early Bathonian).
Telekes Valley—Tributary Valley 8.
In this section seven
samples collected from the black and siliceous shale are re-as-
sessed. The samples yielded the following, relatively well pre-
served and stratigraphically important radiolarian taxa
(Figs. 8, 9): Pseudodictyomitrella spinosa Grill & Kozur,
Canoptum hungaricum Grill & Kozur, Unuma cf. U. typicus
Yao, Parahsuum izeense (Pessagno & Whalen), Transhsuum
hisuikyoense (Isozaki & Matsuda), T. maxwelli (Pessagno), T.
brevicostatum (Ožvoldová), Eucyrtidiellum nodosum Wakita,
E. (?) quinatum Takemura. The co-occurrence of P. izeense
(Pessagno & Whalen) (UAZ 1—3) and T. maxwelli (Pessagno)
(UAZ 3—10) idicates the UAZ 3 (Early—middle Bajocian).
Contrary to Dosztály’s previous data (1994) we could not rec-
ognize any difference in biostratigraphic age between the low-
er and upper part of the investigated sequence. The occurrence
and the stratigraphic distribution of the radiolarians in the ex-
amined samples are shown in Table 1.
Telekesoldal Complex
The TC is made up of shale and marl, sandstone and olis-
trostrome lithofacies. However, their stratigraphic relations
are poorly constrained due to the scarcity of age diagnostic
fossils and continuous successions (Fig. 10). Szalonna Sza-4,
-7, -10, -11, -12, Szendrő Szet-3 and Rudabánya Rb-661 cores
and outcrops on Csehi Hill and the road cut type section at
Telekesoldal provided important data on certain parts of the
complex.
Black shale and clay marl with sandstone layers
One of the typical lithofacies of the TC is made up of dark
grey to black shale and sandstone. Outcrops of this unit oc-
Fig. 8. Determined radiolarian fauna. 1 – Archaeodictyomitra cellulata O’Dogherty, Goričan & Dumitrică; Va-2 borehole: 49.3 m. 2 – Ar-
chaeodictyomitra exigua Blome; Telekes Valley—Tributary Valley 8: 8—43a. 3 – Archaeodictyomitra patricki Kocher; Va-2 borehole: 3.4 m.
4 – Archaeodictyomitra rigida Pessagno; Va-2 borehole: 64.1 m. 5 – Hsuum baloghi Grill & Kozur; Va-2 borehole: 48.5 m. 6 – Hsuum mat-
suokai Isozaki & Matsuda; Va-2 borehole: 73.0 m. 7 – Hsuum mirabundum Pessagno & Whalen; Va-2 borehole: 3.4 m. 8 – Hsuum rose-
budense Pessagno & Whalen; Va-2 borehole: 49.3 m. 9 – Hsuum sp. E in Hull; Va-2 borehole: 58.5 m. 10 – Hsuum cf. cuestaense Pessagno;
Telekes Valley—Tributary Valley 8: 8—47a. 11 – Hsuum cf. sp. 1 O’Dogherty et al.; Telekes Valley—Tributary Valley 8: 8—43a. 12 – Para-
hsuum carpathicum Widz & De Wever; Va-2 borehole: 30.2 m. 13 – Parahsuum indomitum (Pessagno & Whalen); Telekes Valley—Tributary
Valley 8: 8—55a. 14 – Parahsuum officerense (Pessagno & Whalen); Va-2 borehole: 79.1 m. 15 – Parahsuum izeense (Pessagno & Whalen);
Telekes Valley—Tributary Valley 8: 8—47. 16 – Parahsuum snowshoense (Pessagno & Whalen); Va-2 borehole: 64.1 m. 17 – Parahsuum
stanleyense (Pessagno); Va-2 borehole: 3.4 m. 18 – Semishuum inexploratum (Blome); Va-2 borehole: 3.4 m. 19 – Semishuum sp.; Va-2
borehole: 30.2 m. 20 – Transhsuum brevicostatum (Ožvoldová); Telekes Valley—Tributary Valley 8: 8—47a. 21 – Transhsuum hisuikyoense
(Isozaki & Matsuda); Va-2 borehole: 69.7 m. 22 – Transhsuum maxwelli (Pessagno); Va-2 borehole: 64.1 m. 23 – Transhsuum sp. 1; Va-2
borehole: 48.5 m. 24 – Transhsuum sp. 2; Va-2 borehole: 49.3 m. 25 – Dictyomitrella (?) kamoensis Mizutani & Kido; Va-2 borehole:
45.4 m. 26 – Parvicingula sp.; Va-2 borehole: 49.3 m. 27 – Pseudodictyomitrella hexagonata Grill & Kozur; Va-2 borehole: 64.1 m.
28 – Pseudodictyomitrella spinosa Grill & Kozur; Va-2 borehole: 77.6 m. 29 – Pseudodictyomitrella cf. spinosa Grill & Kozur; Va-2 bore-
hole: 77.6 m. 30 – Pseudodictyomitrella wallacheri Grill & Kozur; Va-2 borehole: 77.6 m. 31 – Stichocapsa robusta Matsuoka; Va-2 bore-
hole: 13.1 m. 32 – Stichocapsa sp.; Va-2 borehole: 64.1 m. 33 – Stichocapsa sp. E in Baumgartner; Va-2 borehole: 3.4 m. 34 – Stichomitra sp.;
Va-2 borehole: 49.3 m. 35 – Pseudoeucyrtis elongata Grill & Kozur; Va-2 borehole: 30. 2 m. 36 – Pseudoeucyrtis sp.; Va-2 borehole: 69.7 m.
359
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
360
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
361
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
cur S of the Nagy-Telekes Hill, in the Mély Valley, Balázs-
tető Hill, Csehi Hill (Fig. 1a) and it was also exposed by the
Szalonna Sza-12 core.
The dark shales are actually claymarls and claystones which
contain quartz silt or fine-grained sand scattered in the clay or
forming thin laminae. Erosional bases of the sandstone layers
are common (Fig. 11.2). Graded bedding (Fig. 11.1,2) and
cross-lamination can also be observed within some of the sand-
stone beds. Alternation of fine- to medium-sized sandstone and
sandy siltstone laminae (Fig. 11.2) were also observed in thin
sections. In some samples taken from the Mély Valley alterna-
tion of mm-thick sandstone laminae and thicker silty claystone
layers were found. The sandstones consist predominantly of
quartz, but the amount of feldspars (plagioclases) is usually sig-
nificant and muscovites also occur in varying quantity
(Fig. 11.3). The size of the grains varies from silt to medium-
sized sand. The contacts of the grains are mostly pressure solu-
tion surfaces. Some evidence of intracrystalline deformation is
present. Undulose extinction of the quartz grains is common. In
some grains the recovery reached the last phase: subgrain
boundaries separate the neighbour crystal fragments, which are
slightly misoriented with respect to each other (Fig. 11.3).
Slump folds are commonly visible in the sandstone-bear-
ing successions. Lens shaped sandstone bodies in the shale
are also common. They may have formed either by early
post-diagenetic disintegration of sandstone beds and gravita-
tional redeposition of the sandstone blocks or by subsequent
tectonic deformation processes leading to boudin formation.
Szalonna Sza-12 core.
The Szalonna Sza-12 core exposed
dark grey shale and marl with varying amounts of radiolarian
moulds (calcite and quartz) in its lower part. It is overlain by
a few metre thick interval containing 0.3—20 mm sized grey
clasts with subordinate shale matrix or without any matrix
but microstylolitic grain contacts (olistostrome beds). The
typical components are as follows: “filament” wackestone,
“filament” packstone (coquina), crinoidal wackstone, crinoi-
dal packstone, dolosparite, siltstone, sandy shale, and highly
altered volcanoclasts with quartz and feldspar phenocrystals.
The boundaries between the matrix and the clasts are usually
pressure solution surfaces; dark solution seams of insoluble
material commonly occur around the clasts (Fig. 11.4). The
upper segment of the core section is made up of alternation of
fine-grained siliciclastic sandstone to siltstone and dark grey
shale that can be interpreted as a very distal turbidite se-
quence. Since the original bedding is clearly visible in this al-
ternating sandstone-shale section, the relationship of the S
0—1
foliation and the occurrent fold related axial-plane clevage can
be studied (Fig. 11.5,6). In the sample taken from 37.5 m the
original S
0—1
foliation and the later axial-plane clevage (S
2
) in-
tersect each other at about 70°. This S
2
foliation is spaced, and
defined by anastomosing opaque mineral rich planes.
Dark grey shale and marl with olistostrome layers
Rudabánya Rb-661 core.
In the Rudabánya Rb-661 core
(Fig. 12) the Upper Permian Perkupa Evaporite Formation
and a more than 10 m thick tectonic breccia zone (anhydrite,
black shale, “rauhwacke”) form the basal shear horizon of the
Telekesoldal Nappe (built up by the TC). In this core altered
vitrophyric rhyolite, rhyolite tuff and ignimbrite occur in the
lowermost part of the TC. Under the microscope fragments of
volcanic glass and pumiceous texture – the characteristic fea-
tures of ignimbrite – are clearly visible. Thin laminae of
sericite-chlorite are predominant in the matrix. The porphyrit-
ic components are pertitic orthoclase, idiomorphic quartz with
resorbed margin, fractured quartz with undulatory extinction,
commonly partly melted, and few large sericitic plagioclases
or plagioclase-orthoclase composite grains, and few biotites.
The boundary of the large rhyolite-ignimbrite body (19 m ap-
parent thickness) is sharp. Small (mm to 1 cm-sized) rhyolite
clasts (Fig. 13) were encountered in “spotty” shale (usually
silty claymarl, marl, calcareous marl) in several horizons in a
40 m thick interval above the large body. There are clasts con-
sisting of large quartz and feldspar crystals in a calcified ma-
trix. Composite grains also occur together with resorbed
quartz and orthoclase crystal fragments. There are lithoclasts
consisting of resorbed quartz and sheared, fractured perthitic
orthoclase in a squeezed chloritic, calcitized and silicified ma-
trix. Along with the rhyolite clasts a few carbonate clasts of
similar size were also found. In the sample taken from
101.7 m, radiolarian wackestone (3 cm) (Fig. 14.1), “fila-
ment” wackestone (2 cm) clasts and an altered rhyolite clast
(2 mm) were observed (Fig. 14.2). The typical texture of this
interval is bioclastic wackestone containing large number of
Fig. 9. Determined radiolarian fauna. 1 – Protunuma turbo Matsuoka; Va-2 borehole: 64.1 m. 2 – Unuma ochiensis (Matsuoka); Va-2
borehole: 3.4 m. 3 – Unuma typicus Yao; Va-2 borehole: 64.1 m. 4 – Unuma cf. typicus Yao; Telekes Valley—Tributary Valley 8: 8—43.
5 – Eucyrtidiellum (?) quinatum Takemura; Telekes Valley—Tributary Valley 8: 8—53. 6 – Eucyrtidiellum cf. unumaense (Yao); Va-2 bore-
hole: 64.1 m. 7 – Eucyrtidiellum sp. 1; Va-2 borehole: 51.5 m. 8 – Canoptum hungaricum Grill & Kozur; Va-2 borehole: 69.7 m. 9 – Cano-
ptum rudabanyaense Grill & Kozur; Va-2 borehole: 48.5 m. 10 – Archicapsa sp. 1, Va-2 borehole: 64.1 m. 11 – Archicapsa sp. 2, Telekes
Valley—Tributary Valley 8: 8—47. 12 – Williriedellum sp.; Va-2 borehole: 13.1 m. 13 – Striatojaponocapsa synconexa O’Dogherty, Goričan
& Dumitrică; Va-2 borehole: 13.1 m. 14 – Praewilliriedellum convexum (Yao); Va-2 borehole: 30.2 m. 15 – Praewilliriedellum sp.; Va-2
borehole: 58.5 m. 16 – Laxtorum (?) hichisoense Isozaki & Matsuda; Va-2 borehole: 73.0 m. 17 – Laxtorum (?) jurassicum Isozaki & Matsu-
da; Va-2 borehole: 80.9 m. 18 – Spongocapsula palmerae Pessagno; Va-2 borehole: 58.5 m. 19 – Pantanellium sp. 1; Szet-3: 52.0—53.0 m.
20 – Gorgansium sp.; Szet-3: 52.0—53.0 m. 21 – Cenosphaera sp. X Yao; Szet-3: 69.8—70.6 m. 22 – Acaeniotylopsis (?) sp.; Szet-3:
69.8—70.6 m. 23 – Praeconocaryomma sp.; Va-2 borehole: 69.7 m. 24 – Triactoma cf. jonesi (Pessagno); Szet-3: 52.0—53.0 m. 25 – Triacto-
ma sp. 1; Szet-3: 69.8—70.6 m. 26 – Tetratrabs zealis (Ožvoldová); Va-2 borehole: 73.9 m. 27 – Tritrabs simplex Kito & De Wever; Szet-3:
52.0—53.0 m. 28 – Orbiculiforma sp. X in Baumgartner; Szet-3: 69.8—70.6 m. 29 – Emiluvia lombardensis Baumgartner; Szet-3: 69.8—70.6 m.
30 – Angulobracchia sp.; Va-2 borehole: 69.7 m. 31 – Paronaella sp.; Va-2 borehole: 69.7 m. 32 – Homoeoparonaella elegans (Pessagno);
Szet-3: 52.0—53.0 m. 33 – Homoeoparonaella argolidensis Baumgartner; Szet-3: 52.0—53.0 m. 34 – Bernoullius rectispinus Kito et al.; Va-2
borehole: 48.5 m. 35 – Bernoullius sp., Telekes Valley—Tributary Valley 8: 8—52.
362
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
Table 1:
Presence/absence
of
radiolarian
species
in
Varbóc-2
borehole,
in
Telekes
Valley—Tributary
Valley
8
section
and
in
Szet-3
boreh
ole.
(gr9
=
52.0 m—53.0 m
sample
and
gr11
=
69.8 m—
70.6 m
sample).
Varb
ó
c-
2
(
V
a-
2
) b
o
re
ho
le
(
m
)
S
ze
t-
3
b
h
T
elek
es
Valley — T
rib
ut
ary va
lley 8
UAZ
Tax
a
3.
4
9.
7
13.
1 30.
2
34.
1
45.
4 48.
5
49.
3 51.
5
58.
5 6
4
.1
69.
7
73
73.
9
77.
6
79.
1
80.
9
gr9
gr11
8-
43
8-
43a
8
-47
8-
47A
8-
51
8-
52
8-
53
8-
55a
A
caenio
tyl
ops
is
(?
) s
p
.
+
+
A
cantho
c
ir
cus
(?
) s
p
.
+
+
+
3–10
A
ngul
ob
ra
cchia digit
a
ta
Ba
u
m
g
ar
tn
er
+
A
ngul
ob
ra
cchia
sp
.
+
+
Ar
chae
o
d
ic
ty
om
itr
a c
ellulata
O’
Do
gh
er
ty
,
Gor
ič
an
&
Du
m
it
ri
că
+
+
A
rchaeo
d
ictyom
itr
a exigua
Bl
o
m
e
+
+
+
+
A
rchaeo
d
ictyom
itr
a patr
icki
Koc
h
er
+
A
rchaeo
d
ictyom
itr
a pr
is
ca
Ko
z
u
r &
M
o
st
le
r
+
A
rchaeo
d
ictyom
itr
a r
igida
P
essag
n
o
+
+
Ar
chae
o
d
ic
ty
om
itr
a
sp
. 1
+
+
Ar
chae
o
d
ic
ty
om
itr
a
sp
. 2
+
Ar
chae
o
d
ic
ty
om
itr
a
sp
. 3
+
Ar
ch
ic
a
p
sa
sp
. 1
+
+
+
+
Ar
ch
ic
a
p
sa
sp
. 2
+
Ar
ch
ic
a
p
sa
sp
. 3
+
B
agot
um
sp
.
+
1–9
B
er
noull
iu
s r
ectis
pinus
Ki
to et a
l.
+
B
er
noull
iu
s
sp
.
+
C
anoptu
m
hung
ar
icum
Gr
ill
&
K
o
z
u
r
+
+
+
+
+
+
+
C
anoptu
m
cf
. hungar
icum
Gr
ill
& K
o
z
u
r
+
C
anoptu
m
r
udabanyae
ns
e
Grill
& K
o
z
u
r
+
C
anoptu
m
sp
.
+
C
anoptu
m
(?
) sp
.
+
1–4
C
enos
ph
aer
a
sp
. X
Y
ao
+
Cyrt
o
ca
p
sa
sp
.
+
3–7
Dic
ty
o
m
itr
ella
(?
)
kamoensi
s
Mi
z
u
ta
n
i &
K
id
o
+
+
1–4
E
m
iluvi
a
lombar
dens
is
B
a
u
m
g
ar
tn
e
r
+
+
1–4
Emiluv
ia
c
f.
lombar
dens
is
B
a
u
m
g
a
rt
n
er
+
Emiluv
ia
sp
.
+
Emiluv
ia
(?
) sp
.
+
+
+
3–10
E
u
cyr
tid
iell
um nodos
um
Wak
it
a
+
+
+
Euc
yr
tid
ie
ll
um
(?
)
quina
tum
Ta
k
e
m
u
ra
+
+
Euc
yr
tid
ie
ll
um
cf
.
unumaens
e
(Y
ao
)
+
Euc
yr
tid
ie
ll
um
sp
. 1
+
+
+
+
Euc
yr
tid
ie
ll
um
sp
. 2
+
5–8
Euc
yr
tid
ie
ll
um
c
f.
unumaens
e pus
tulatum
B
a
u
m
ga
rt
ne
r
+
Gor
gans
ium
sp
.
+
4–11
Homoeo
par
onael
la ar
golidens
is
B
a
u
m
g
ar
tn
e
r
+
+
4–10
Homoeo
par
onael
la elegans
(
P
es
sa
gno)
+
Homoeo
par
onael
la
? sp
.
+
+
Hs
uum b
a
loghi
Gr
ill
& K
o
z
u
r
+
Hs
uum b
elliatulu
m
Pes
sa
gn
o & W
h
a
le
n
+
Hs
uum
cf
. be
lliat
u
lum
Pes
sa
gn
o & W
h
a
le
n
+
1–5
Hs
uum m
a
ts
uokai
I
sozak
i &
Mat
su
d
a
+
+
+
+
Hs
uum
cf
.
mats
uokai
Is
ozak
i &
Mat
su
d
a
+
363
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Table 1:
Continued.
V
a
rb
ó
c-2
(V
a
-2
) b
o
re
ho
le
(
m)
S
ze
t-3
b
h
T
elek
es
Valle
y — T
rib
ut
ary
va
lley 8
UAZ
Tax
a
3.
4
9.
7
13.
1
30.
2 34.
1
45.
4 48.
5
49.
3
51.
5
58.
5
64.
1 69.
7
73
73.
9
77.
6
79.
1
80.
9
gr9
gr11
8-
4
3
8-
43a
8-
47
8
-47A
8-
51
8-
52
8-
53
8-
55a
3–6
Hs
uum mir
abun
dum
Pes
sa
gno &
W
h
a
le
n
+
+
+
+
+
Hs
uum
cf
. mir
a
bundu
m
Pes
sa
gno & W
h
a
le
n
+
Hs
uum r
o
se
bud
ens
e P
es
sa
g
n
o
&
Wh
al
en
+
Hs
uum
sp
. E
se
n
su
H
u
ll
+
Hs
uum
cf
. sp
. 1
sen
su
O
’D
o
g
h
e
rt
y
et
a
l.
+
+
Hs
uum
cf
.
cues
ta
ense
P
essag
n
o
+
Hs
uum
cf
.
robu
st
um
Pes
sa
gno &
Wh
a
le
n
+
Hs
uum
sp
. 1
+
+
+
Hs
uum
sp
. 2
+
Hs
uum
(?
) s
p
.
+
1–4
Laxtor
um
(?
) h
ichis
oens
e
Is
oz
ak
i & M
ats
uda
+
+
+
+
Laxtor
um
(?
) c
f.
hichis
oens
e
Is
o
za
k
i & M
ats
u
d
a
+
+
+
2–3
Laxtor
um
(?
)
ju
ra
ssi
cu
m
Is
oz
ak
i & M
ats
u
d
a
+
+
Laxtor
um
(?
) sp
.
+
+
1–6
Or
bic
u
lifor
m
a
sp
. X
sen
su
B
a
u
m
g
art
n
er
+
+
Or
bic
u
lifor
m
a
sp
.
+
P
anta
n
ellium
s
p
. 1
+
P
anta
n
ellium
s
p
. 2
+
P
a
ronaella
sp
. B
sen
su
H
u
ll
+
P
a
rahs
uum car
pathicum
Wi
d
z
&
D
e W
ev
er
+
P
a
rahs
uum ind
o
m
itum
(P
es
sa
gno & W
h
a
le
n
)
+
1–3
P
a
rahs
uum iz
ee
ns
e
(P
es
sa
g
n
o
&
Wh
al
en
)
+
1–7
P
a
rahs
uum offi
cer
ens
e (
P
es
sa
gn
o
&
W
h
al
en
)
+
P
a
rahs
uum
cf
. of
fi
cerense
(
P
es
sa
g
n
o
&
Wh
al
en)
+
P
a
rahs
uum s
n
o
w
sh
oens
e
(P
es
sa
gn
o & W
h
al
e
n
)
+
+
3–8
P
a
rahsuum st
a
n
leyense
(P
essag
n
o
)
+
P
a
rahs
uum
sp
.
+
P
a
ronaella mu
ll
er
i
P
essag
n
o
+
1–2
P
a
ronaella
c
f.
corpul
ent
a
D
e W
e
v
er
+
+
P
a
ronaella
sp
.
+
P
a
ronaella
(?
) s
p
.
+
P
a
rv
icingul
a
cf
. elegans
P
essag
no &
Wh
a
len
+
P
a
rv
icingul
a
sp
.
+
+
P
raeconocar
yo
mma
sp
.
+
1–11
P
rae
w
illir
iedel
lu
m convexum
(Y
ao
)
+
+
+
P
rae
w
illir
ie
de
ll
u
m
sp
.
+
P
rotunum
a cos
tata
(H
e
it
zer
)
+
4–7
P
rotunum
a tur
b
o
M
ats
u
oka
+
+
+
+
+
P
rotunum
a
sp
.
+
+
P
rotunum
a
(
?)
sp
.
+
P
seu
docrucel
la
(?
) sp
.
+
P
seu
doeucyrt
is
buekkensi
s
Gril
l &
K
o
z
u
r
+
P
seu
doeucyr
tis
elongata
Gr
ill
&
K
o
z
u
r
+
P
seu
doeucyrt
is
sp
.
+
+
+
P
seu
dodictyom
itr
ella hexagona
ta
(
H
e
it
zer
)
+
P
seu
dodictyom
itr
ella s
p
inos
a
G
rill
&
K
o
z
u
r
+
+
+
+
+
P
seu
dodictyom
itr
ella
cf
. s
p
inos
a
Gr
ill
&
Koz
u
r
+
+
P
seu
dodictyom
itr
ella w
a
llacher
i
Gr
ill
& Koz
u
r
+
+
Semihs
uum fuc
h
si
(Gr
ill
& K
o
z
u
r)
+
+
364
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
Table 1:
Continued.
V
a
rb
ó
c-2
(V
a
-2
) b
o
re
ho
le
(
m
)
S
ze
t-3
b
h
T
elek
es
Valley —
T
rib
ut
ary va
lley 8
UAZ
T
a
x
a
3.
4
9.
7
13
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365
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Fig. 10. Simplified reconstructed stratigraphic column of the Tele-
kesoldal Complex. The stratigraphic positions of the age data, the
studied boreholes and outcrops are approximately indicated.
radiolarians recrystallized to calcite, probably also sponge spi-
cules and small fragments of thin-shalled bivalves (“fila-
ments”) locally. Darker bioturbation patches rich in organic
matter and pyrite are common.
The shale is commonly strongly squeezed and deformed.
Pressure solution seams are common in this interval
(Fig. 14.5). The original sedimentary texture is punctuated by
pressure solution seams which are commonly rich in opaque
solution residual material. The contact between the shaly ma-
trix and the occasionally present clasts are usually pressure so-
lution surfaces, too. They are rich in insoluble material. The
layer-perpendicular shortening is clearly visible in the case of
the presence of originally subround shaped bioclasts (radi-
olarians) (Fig. 14.4). Signs of at least two phases of ductile
deformation could be recognized in the thin sections. The
sample from 96.1 m contains very tight, almost isoclinal
folds, formed by the original radiolarian layers (Fig. 15.1).
An incipient axial plane clevage (S
2
) is connected to this
folding phase. At 19.5 m a few mm scale kink fold (F
3
)
bends the original bedding or previous foliation (Fig. 15.2).
The fold has angular hinge, the limbs meet each other at a
sharp line. Tension joints syndeformationally filled with cal-
cite are frequent in the hinge zone, while the bedding or pre-
vious foliaton planes worked as sliding surfaces. This
deformation took place at the transition of ductile and brittle
deformation fields.
In spite of the later deformation the original sedimentary
texture can be recognized. It may have been radiolarian
wackestone originally, but calcite moulds are more or less
deformed, the globular moulds became lens shaped, and the
bioturbation patches also got flattened. Only slightly squeezed
and deformed shale also occur in several horizons, rarely. In
the upper part of the sequence (above 100 m) the spotty
shale (marl, silty marl) lithology and the radiolarian wacke-
stone texture continues but the clasts are missing, whereas in
the uppermost ~ 40 m of the core section the barren mud-
stone texture is prevailing. In a single sample at 25.0 m,
probably representing a larger clast, well preserved thin-
shalled bivalve fragments (Fig. 14.3) were found in silicified
marl matrix (“filament” wackestone).
Hunter House section.
In the neighbourhood of the Hunter
House in the Telekes Valley slightly melted plagioclase free
granite cataclasite was found within the rhyolite (Fig. 16.1).
Szalonna Sza-10 core.
Rhyolites within a marl and clay-
stone succession were also encountered in the Szalonna Sza-10
core (Grill 1988). An olistostrome layer containing predomi-
nantly radiolarian wackestone (Fig. 16.2), radiolarian—“fila-
ment” wackestone and a single, probably platform-derived
clast (Fig. 16.3,5) was found in the 95.4—95.5 m interval.
These platform facies carbonate clasts are very rare in the olis-
tostrome of the TC. In core Sza-11 36.5—57.25 m along with
the radiolarian “filament” wackstone, coarsely crystalline do-
losparite and shale lithoclasts, an oolitic-crinoidal packstone
clast was found in a shale matrix (Fig. 16.4,6).
Szalonna-Perkupa road cut key-section.
The road cut
key-section along the road between Szalonna and Perkupa is
the best exposure of the typical olistotrome lithofacies
(Kovács 1988). In the exposed succession 1—5 m thick dark
greenish-grey bioturbated marl beds alternate with 0.1—5 m
thick olistostrome beds. Centimeter- to tens of centimeters-
sized clasts (mostly grey limestone and green rhyolite clasts)
occur in the olistostrome beds (Fig. 17.1). The original
shapes of the limestone and rhyolite clasts are rarely visible
due to pressure solutional grain contacts and tectonic defor-
mation. Angular brownish shale clasts, 0.5—2 cm in size, also
commonly occur. The thickest beds contain the coarsest
grains where size of rhyolite clasts may reach 0.5 m in diam-
eter (Kovács 1988). Grain supported texture is typical but
mud-supported debris flow deposits are also present, rarely.
In the grain-supported beds the matrix is usually missing or
subordinate, the microstylolitic grain contacts are typical.
366
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
The other characteristic feature for pressure solution here is
the displacement of layering on certain planes (Fig. 17.2). In
the matrix supported olistostromes the matrix is dark shale,
marl with organic material and pyrite or fine siliciclastics
with altered volcanogenic components.
In the olistostrome beds the carbonate clasts are predomi-
nant, their typical texture types are as follows: thin-shelled
Fig. 11. 1 – Radiolarian turbidites. 2 – Erosional base and normal gradation of the sandstone and siltstone beds. 3 – Signs of intracrystal-
line deformation: undulose extinction of the quartz grains, subgrain boundaries separate the neighbouring crystal fragments. 4 – Carbonate
lithoclast with shale matrix. At the rim of the clast dark seams consisting of insoluble material concentrated during dissolution are visible.
5, 6 – Presence of F
2
fold in the alternating sandstone-shale section. The original S
0—1
foliation (subvertical on photo) and the later axial-plane
clevage (S
2
) intersect each other at about 70°. This S
2
foliation is spaced, and defined by anastomosing opaque mineral rich planes. Sza-12, 37.5 m.
bivalve (“filament”) wackestone, radiolarian and “filament”
wackestone, bioclastic (crinoidal), peloidal wackestone, pe-
loidal grainstone, crinoidal wackestone, radiolarian wacke-
stone, micritic mudstone (partially dolomitized or silicified
in some cases), oolitic crinoidal packstone, dolomicrosparite
and dolosparite, sparry calcite, and pervasively silicified
rock. Some platform derived carbonate clasts were also de-
367
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Fig. 12. Reconstructed lithological and stratigraphic features of the
Rudabánya Rb—661 borehole. Note tectonically reduced pelagic
Bódva Triassic below the evaporite, underlain by (Bódva?) platform
carbonate.
tected. Early Ladinian to Late Norian conodonts were found
in some grey limestone clasts (Balogh & Kovács 1977). The
predominant part of the carbonate clasts is probably Triassic
in age, and represents hemipelagic facies.
The sample presented on Fig. 17.3,5 is a succession, start-
ing with greenish grey silty claystone basin facies. Above an
uneven erosional surface, it is overlain by a 2 cm thick litho-
clastic, bioclastic packstone layer with subordinate mi-
crosparitic matrix (Fig. 17.3). The typical grain size is be-
tween 1—5 mm, no grading is visible. The bioclasts are coarse
sand-sized crinoid ossicles. The types of lithoclasts are as fol-
lows: bioclastic wackestone, peloidal wackestone, peloidal
microsparite with a few “filaments”, dolosparite and silty
claystone (yellow). This layer is overlain by a 1 cm thick
sponge spicule packstone (partially silicified) (Fig. 17.4) that
is followed by a turbidite layer with an erosional contact. The
~
1 cm thick allodapic layer is lithoclastic crinoidal packstone
showing definite grading (Fig. 17.5).
Along with carbonate clasts highly altered volcanoclasts are
usually common. Holocrystalline locally spherulitic, porphy-
ritic rhyolites are typical (Fig. 18.1). They contain perthitic or-
thoclase, quartz of undularory extinction and idiomorhic
resorbed quartz (Fig. 18.2), commonly surrounded by a sili-
ceous ring. Strongly altered intersertal-intergranular basalt-
dolerite clasts with slightly bent plagioclase lathes were also
encountered rarely (Fig. 18.3—4). Individual idiomorphic re-
sorbed quartz grains, mosaic like quartz crystals or crystal
stacks, sericitic orthoclase and rarely plagioclase (oligoclase)
derived from volcanites, together with coarse sand-sized
crinoid ossicles also occur in some samples.
Range between the Telekes and Henc Valleys.
Partially
silicified carbonates containing carbonate lithoclasts were
found in some samples taken from outcrops on the range
between the Telekes Valley and Henc Valley. The texture
is lithoclastic grainstone. Along with the 1—2 mm sized,
medium to well rounded lithoclasts coarse sand-size bio-
clasts (bivalve and echinoderm fragments) also occur, rare-
ly. The composition of the lithoclasts is as follows: micritic
and microsparitic mudstone, “filament” wackestone, radi-
olarian wackestone and totally silicified clasts.
Revision of the radiolarian fauna in Telekesoldal Complex
Szet-3 borehole.
Two samples (sample at 52.0 m—53.0 m
and sample at 69.8 m—70.6 m) from the borehole yielded
moderately well preserved and relatively abundant radiolari-
an assemblages, mainly characterized by spumellarians. The
following stratigraphically important radiolarians were iden-
tified from the sample at 69.8 m—70.6 m (Fig. 9): Emiluvia
lombardensis Baumgartner, Emiluvia spp., Unuma cf. typi-
cus Ichikawa & Yao, Laxtorum (?) jurassicum Isozaki &
Matsuda, Triactoma spp., Pseudoeucyrtis sp., Orbiculiforma
sp. X sensu Baumgartner et al. The biostratigraphic range of
E. lombardensis Baumgartner indicates UAZ 1—4 and L. (?)
jurassicum Isozaki & Matsuda indicates UAZ 2—3. Co-oc-
currence of these species and the presence Unuma cf. typicus
Ichikawa & Yao (UAZ 3—4) indicates that this sample can be
assigned to UAZ 3 (Early—middle Bajocian).
The sample from 52.0 m—53.0 m yielded moderately well
preserved and diversified radiolarian fauna (Fig. 9) including
Pseudodictyomitrella spinosa Grill & Kozur, Transhsuum
cf. maxwelli (Pessago), Homoeoparonaella argolidensis
Baumgartner, Homoeoparonaella elegans (Pessagno), Ho-
moeoparonaella cf. elegans (Pessagno), Unuma sp. F sensu
Yao, Gorgansium sp., Pantanellium sp., Tritrabs simplex
Kito & De Wever, Tritrabs cf. ewingi (Pessagno), Emiluvia
368
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
Fig. 13. 1 – Rock fragment surrounded by fibrous calcitic cement and containing large, fragmented quartz and smaller K-feldspar crystals
in a sheared fine-grained, mostly sericitized matrix. Crossed polars, Rb-661, 116.1 m. 2 – Boundary of siltstone and sheared carbonatized
rock fragment, in which large quartz, K-feldspar opaque minerals and few biotite crystals are surrounded by totally chloritized, sericitized
glassy matrix. 1 polar, Rb-661, 149.0—149.1 m. 3 – Sheared, carbonatized rock fragment containing large quartz and K-feldspar crystals
with diffuse boundary in siltstone. Crossed polars, Rb-661, 132.6 m. 4 – K-feldspar, quartz and biotite in glassy groundmass with charac-
teristic texture of pumice bearing rhyolite tuff (ignimbrite). 1 polar, Rb-661, 153.3 m. 5 – Irregular shaped rock fragment with angular
quartz crystals and sparitic matrix in siltstone. Crossed polar, Rb-661, 108.8 m. 6 – Large, slightly deformed and altered plagioclase (most
probably albite) crystal in glassy groundmass, + polar, Rb-661, 153.3 m.
lombardensis Baumgartner, Triactoma cf. jakobse Carter,
Pseudocrucella? sp., Paronaella cf. corpulenta De Wever,
Angulobracchia digitata Baumgartner, Hsuum fuchsi Ko-
zur. The biostratigraphic range of E. lombardensis Baum-
gartner indicates UAZ 1—4, while H. argolidensis Baum-
gartner, H. elegans (Pessagno) indicate UAZ 4—11. It fol-
lows that co-occurrence of them indicate the UAZ 4 (Late
Bajocian).
369
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Fig. 14. 1 – Radiolarian wackestone intraclast in radiolarian
wackestone matrix containing much less radiolarian moulds than
the clast. Note the microstylolitic grain boundaries. Rb-661,
113.0 m. 2 – Rhyolite fragment consisting of holocrystalline mo-
saic like carbonatized quartz matrix and resorbed idiomorphic por-
phyric quartz crystal embedded in fine-grained silty matrix, 1 polar.
Rb-661, 101.7 m. 3 – Thin-shalled bivalves in partially silicified
micritic matrix – “filament” wackestone. Most probably it is a
large lithoclast in the shale that was found below and above this in-
terval. Rb-661, 25.0 m. 4 – Indicator of the strong layer-perpendic-
ular shortening by means of the originally subround shaped bioclast
and flattened radiolarians. 5 – Clearly visible pressure solution
seams in coarse-grained turbiditic layers (with crinoid fragment) of
Telekesoldal Complex.
Palynological age determination
Three wells (Sza-10, Sza-12, Szö-3) (Fig. 1) were sampled to
analyse the sedimentary organic matter content. The Bajocian
age of the dark shales of the TC based on the radiolarian fauna
is confirmed by first findings of marine palynomorphs within
this member. Sample 76.0 m from well Szö-3 yielded poorly to
moderately preserved sedimentary organic particles. Poorly pre-
served specimens of the dinoflagellate cyst Nannoceratopsis
gracilis Alberti were identified. This finding confirmed not only
the Bajocian age, but also the structural position of this sample,
because it proved that the dark shale of Szö-3 belongs to the
TC. Other evidence (style of deformation, metamorphic temper-
ature and pressure data) will be presented in a later paper.
Age-diagnostic dinoflagellate cysts (Wanaea sp., Ctenido-
dinium sp.) were also detected in sample 50.3 m from well
Sza-12, indicating a Callovian age. Sample 74.0 m from well
Sza-10 is characterized by opaque phytoclasts only; no pa-
lynomorphs are preserved.
Csipkés Hill olistostrome
Olistostrome, graded calcarenite and mixed siliciclastic—
carbonate sandstone beds crop out on the southern slope of
370
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
Csipkés Hill. The section starts with alternating marl and
coarse-grained carbonate sandstone beds, which are fol-
lowed by upward coarsening bundles of olistostrome beds.
Macroscopically the calcarenite beds show normal grada-
tion. The contacts between the marl and carbonate sandstone
layers are usually undulate erosional surfaces.
Microscopically these graded carbonate turbidites are
made up of mm-thick microlayers. Lithoclastic, bioclastic
packstone of medium arenite grain size alternates with fine-
grained lithoclastic peloidal grainstone. “Filament” wacke-
stone and packstone, radiolarian wackestone and dark brown
limonitic sparites are the typical lithoclast types. Crinoid os-
sicles and foraminifers occur in the interparticle micritic or
microsparitic to fine sparitic material (Fig. 19). The follow-
ing foraminiferal assemblage was encountered: Planiinvolu-
ta sp., Trochammina sp., Siphovalvulina sp., Valvulina sp.,
Tubinella? sp., Eoguttulina sp. and Nodosaria sp., Callorbis
minor Wernli & Metzger, Protopeneroplis striata Weyn-
schenk (Fig. 20). In case of the latter two species due to
strong recrystallization and partial dissolution of the calcite
wall of the foraminifers the sections do not show the charac-
teristic features. Callorbis minor has been known exclusive-
ly from the Bajocian but it was reported only from a few
places (Wernli & Metzger 1990; Bassoullet 1997; Piuz
2004). It was also encountered in the Bükkzsérc Limestone
in core Bükkzsérc Bzs-5 (Haas et al. 2006). The stratigraphic
range of the Protopeneroplis striata is Late Aalenian—Late
Tithonian (Schlagintweit & Ebli 1999; Schlagintweit et al.
2008). The range of Siphovalvulina is Hettangian to Early
Cretaceous (Kaminski 2004). Consequently the Jurassic dep-
ositional age of the beds is proven and a Middle Jurassic
(Bajocian?) age for the exposed beds is highly probable.
The upper part of the section contains olistostrome hori-
zons. Macroscopically the olistostromes are grain supported,
containing clasts from 1—2 mm to 4—5 cm in size. They are
poorly sorted; the size of the clasts may vary in the same layer
between a few mm-s and a few cm-s. The visible clasts are
usually well-rounded. The following components could be
distinguished by the naked eye: pink, red, light grey and black
limestones, grey and green marl, red and light grey cherts.
In microscopic view the investigated olistostrome sample
contains a large amount of lithoclasts, 1—3 cm in size. The
following lithoclasts could be recognized: thin-shelled bi-
valve (“filament”) coquina, radiolarian—“filament” wacke-
stone, calcitized radiolarite, silicified “filament” wackestone,
peloidal wackestone—packstone, clotted micrite with shrink-
age pores that contains foraminifers and, brown carbonate
grains with limonite staining. Lithoclastic, crinoidal pack-
stone with fine arenite-sized grains that is either a layer or
larger lithoclast was also observed (Fig. 19).
Lithoclastic packstone containing 1—3 mm sized lithoclasts in
a microsparitic matrix (micro-olistostrome) is another typical
texture of the exposed succession. The lithoclasts are slightly
rounded to well-rounded. “Filament” wackestone and pack-
stone, radiolarian wackestone, micritic mudstone, silicified “fil-
ament” packstone and chert are the typical components.
Discussion
Interpretation of the lithofacies units of the Telekesvölgy
Complex
Based on data discussed above our summarizing conclu-
sions are as follows:
The Norian Hallstatt Limestone – well dated by con-
odonts – gets more argillaceous upward and gradually
progresses into reddish to greenish and then grey marl that
may correspond to the latest Triassic Zlambach Formation.
Middle to Late Triassic pelagic limestone olistoliths – that
is, slided blocks lithologically similar to the underlying stra-
ta – occur in the variegated marl unit, locally. These blocks
could break down from the footwall of normal faults, con-
necting to the ongoing tectonic processes. The presence of
shallow-water foraminifers (Perkupa-74 core) in this base-
of-slope environment most probably refers to turbiditic cur-
rents, transporting platform derived material into the basin.
The age of this variegated marl is Norian—Rhaetian (?).
The stratigraphic relationship between the previously de-
scribed formation and the pelagic basin facies radiolarian
Fig. 15. 1 – Very tight, almost isoclinal folds, formed by the corser-grained layers in Rb-661 core, 96.1 m. 6 – A few mm scale kink fold
(F
3
) bends the original bedding or previous foliation. The original texture may have been radiolarian wackestone. Rb-661, 19.5 m.
371
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Fig. 16. 1 – Slightly melted plagioclase free granite cataclasite within the rhyolite of Telekesoldal Complex (TC) from the neighbourhood
of the Hounter House in the Telekes Valley. 2 – Radiolarian wackestone and radiolarian “filament” wackestone components of the TC
olistostrome. Sza-10, 95.4 m. 3, 5 – A rare platform-derived clast containing a foraminifers (in the white circle) and moulds, filled with
coarsely crystalline sparite. Sza-10, 95.4 m. 4, 6 – A unique ooidal-crinoidal packstone texture clast from the TC olistostrome. Sza-11,
36.5 m. The white boxes on 3 and 4 indicate the enlarged areas (5, 6).
wackestones (unknown age) of similar lithological composi-
tion and colour – explored in Rb-658 core – is not evi-
denced.
The variegated marl gradually progresses into grey marl
and calcareous marl, containing significant amount of rede-
posited crinoid fragments. Accordingly it may be interpreted
as a hemipelagic facies, relatively close to submarine highs.
The age of this lithofacies unit is also unknown.
The black shale, rich in radiolarians and sponge spicules
is a typical deep pelagic basin facies, Bajocian to Early Ba-
372
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
thonian in age. The stratigraphic relationship of this lithofa-
cies unit with the previously described one is not proven.
Interpretation of depositional conditions of the Telekesoldal
Complex
The sedimentological characteristics of the sandstone
layers such as alternation of shale and sandstone layers,
erosional base of the sandstone layers and slump folds indi-
cate their turbiditic origin. The sandstone-bearing shale
lithofacies was formed in a relatively deep pelagic basin
that was reached by proximal to distal siliciclastic turbidity
currents. The sand to silt-size siliciclastic material can be
derived from a distal provenance and multiple redeposi-
tions of fine siliciclasts via river—delta—deep sea fan can be
assumed.
Fig. 17. 1 – Olistostrome from the road cut key-section along the road between Szalonna and Perkupa. The olistostrome is grain support-
ed, the clasts are centimeter- to tens of centimeters-sized (mostly grey limestone and green rhyolite clasts). 2 – A characteristic feature for
pressure solution: displacement of layering on certain planes in the Telekesoldal Complex olistostrome. 3—5 – Greenish grey silty claystone
basin facies is erosionally overlain by a 2 cm thick lithoclastic, bioclastic packstone layer (3). It is overlain by a 1 cm thick sponge spicule
packstone (partially silicified) layer (4), which is followed by a turbidite layer (lithoclastic crinoidal packstone (5)).
373
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
The coarse-grained gravity deposits (debrites, coarse grain
turbidites) must have been accumulated close to the slope.
The carbonate components (extraclasts) of the gravity flow
deposits (olistostromes) are predominantly Middle to Late
Triassic (Kovács 1988) pelagic limestones showing features
of the grey Hallstatt (Pötschen) facies (radiolarian and “fila-
ment” wackestones), crinoidal limestones and rarely lime-
stones of reworked platform facies. The age of the
radiolarian wackestone and mudstone clasts is ambiguous
(Triassic or Jurassic or both). Rhyolite volcanoclasts and re-
lated quartz and feldspar grains are also common and typical
components of the gravity mass flow deposits. The rhyolitic
clasts are derived both from lava rocks and ignimbrites.
They contain large perthitic orthoclase and fractured quartz
of undulating extinction which may derive from assimila-
tion, partial melting of acidic to neutral intrusive rocks.
Smaller amounts of sericitic plagioclase accompany this as-
semblage locally, rock inclusions showing intrusive rock
texture and consisting of these kinds of feldspar also occur,
rarely. The large rhyolite-ignimbrite olistolith at the base of
the Jurassic succession (Rb-661 and Sza-10 cores), implies a
close volcanic source area and base-of-slope depositional
setting. The higher part of the exposed section where smaller
rhyolite clasts and various carbonate lithoclasts occur indi-
cates decreasing slope related redeposition, and more distal
slope-related setting. We have no relevant radiometric age
data for these volcanic rocks.
The lithological features described above imply a relative-
ly deep marine basin in the proximity of a submarine slope
as the depositional environment of these lithofacies units.
The typical components of the olistostromes indicate that the
Triassic and probably Jurassic carbonates formed on an at-
tenuated continental crust (Hallstatt facies zone) and volca-
nic rocks (probably Jurassic) must have been present in the
source area of the gravity flows. Poor rounding of the coarse
grains implies an escarpment as the primary source of the
clasts; accordingly fluvial transportation prior to the gravity
redeposition cannot be considered as a realistic model. Com-
pressional tectonics leading to nappe stacking of the ocean
margin may have created suitable conditions for this sedi-
mentation pattern. Nappe stacking brought superposition of
Triassic pelagic carbonates and volcanic formations. These
Fig. 18. 1 – Rhyolite fragment with holocrystalline partly spherulitic matrix, rounded quartz and large K-feldspar crystalls. Crossed polars, Tele-
kesoldal key section. 2 – Resorbed quartz and large K-feldspar crystals in a strongly carbonatized fragment, in a carbonate rich olistostrome.
Crossed polars, Telekesoldal key section. 3 – Strongly altered opacitized and carbonatized intersertal basalt fragment with skeletal structured
laths of plagioclase and some parallel shearing zones. 1 polar, Telekesoldal key section. 4 – Strongly altered opacitized and carbonatized interser-
tal basalt fragment with skeletal structured laths of plagioclase, calcite and limonitized magnetite aggregates. 1 polar, Telekesoldal key section.
374
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
movements led to formation of steep slopes and intense tec-
tonics caused fragmentation of hard rocks and triggered
gravity mass movements. The coarse gravity deposits
formed slope apron along the foreland of the thrust belt in a
subduction related basin.
The above described mainly calc-alkalic volcanic associa-
tion may have derived from a coeval suprasubduction in a
Fig. 19. Detailes of calciturbidite layers from Csipkés Hill olis-
tostrome. Lithoclastic, bioclastic packstone of medium arenite grain
size (1) alternates with fine-grained lithoclastic peloidal grainstone
(2). “Filament” wackestone and packstone, radiolarian wackestone
and dark brown limonitic sparites are the typical lithoclast types (3).
magmatic arc. It is evident that in the TC the rhyolites are
predominant among the volcanoclasts, while the basalt clasts
are rare. However, no relevant geochemical analysis has
been performed on the basalt clasts, so far.
The depositional area must have been in the vicinity of the
ongoing nappe stacking of the thinned continental margin in
connection with the Middle—Upper Jurassic subduction and
obduction processes of the Neotethys Ocean (Schmid et al.
2008). However, the coeval exitence of a suprasubduction
magmatic arc system, that may have acted as a source area of
the rhyolite clasts and blocks, has not yet been proven due to
the lack of relevant radiometric age data.
The depositional environment, stratigraphic and tectonic
position of the Csipkés Hill olistostrome
On basis of their microfacies pattern, the above mentioned
components are derived most probably from the formations
of the Middle to Upper Triassic Hallstatt facies. However,
the light grey limestone clasts of peloidal wackestone—pack-
stone texture and clotted micrite with shrinkage pores tex-
ture, may have originated from platform limestone, likely
from the Anisian Steinalm Limestone. The red cherts (the
calcitized radiolarites found in thin sections, too) and pink
limestones with thin-shelled bivalve (“filament”) coquina
are possibly equivalent to the Ladinian to Carnian Bódvalen-
ke Limestone (red cherty limestone). The dark grey or black
cherty limestones (radiolarian wackestone, micritic mud-
stone in thin sections) may have been derived from the Bód-
varákó Formation (dark grey cherty limestone and marl).
These coarse-grained gravity deposits must have been ac-
cumulated close to a slope. The typical components of the
olistostromes indicate that Middle to Upper Triassic carbon-
ates formed in the Hallstatt facies zone must have been
present in the source area of the gravity flows.
Taking into account that a shallow-marine carbonate plat-
form was the habitat of Siphovalvulina and Protopeneroplis,
and platform foreslope to deeper shelf of Callorbis minor
these fossils must have been derived from a penecontempo-
raneous active platform just like in the case of the similar
genera found in the Bükkzsérc Limestone in the Mónosbél
Complex in the Bükk Mts (Haas et al. 2006).
However, both the stratigraphic and the tectonic position
of the Csipkés Hill olistostrome are quite uncertain; from a
tectonic point of view it is likely to be part of the Telekes-
völgy Complex. The main reasons are the lack of metamor-
phic overprint and ductile deformation, which are the
characteristic features of the TVC in contrast with the TC
(Kövér et al. 2007). However, the sedimentary features
(gravity mass transport, olistostrome horizons, and turbid-
ites) and supposed depositional environment (slope) shows
greater similarity to the TC, than the mostly basinal facies of
the TVC. Accordingly, the olistostrome and carbonate tur-
bidite beds of Csipkés Hill were deposited close to a slope
like the sediments of the TC, but they did not form in the same
(or in the same part of this) basin, because the clastic compo-
nents and accordingly the source areas (red and grey Hallstatt
facies zones) and the further structural evolution (ductile de-
formation, metamorphism) are completely different.
375
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
Comparison
The formation of the Jurassic complexes exposed in the
Rudabánya Hills can be related to the evolution and mostly
to the closure of the westernmost sector of the Neotethys
Ocean. Complexes showing more or less similar features
and evolution occur north of our study area near to Meliata
and Jaklovce villages, Slovakia (Meliaticum) (Kozur et al.
1996; Mock et al. 1998) and also south of the Rudabánya
Hills, in the Darnó-Bükk area, North Hungary (Haas &
Kovács 2001; Haas et al. 2006). Both areas are close to the
Rudabánya Hills; however the former one shows affinity
with parts of the “Hallstatt Mélange” in the Northern Cal-
careous Alps (Kozur & Mostler 1992; Gawlick et al. 1999,
2002; Frisch & Gawlick 2003; Gawlick & Frisch 2003),
whereas the latter one is probably of Dinaric origin (Vardar
Zone and Dinaridic Ophiolite Belt) (Karamata et al. 2000;
Pamić et al. 2002; Dimitrijević et al. 2003; Karamata
2006). Therefore the aim of the comparison is to decide
which of these complexes show closer affinity with those
in the Rudabánya Hills.
Western Carpathians – Meliata Unit
There are two important occurrences of the Meliata Unit in
SE Slovakia. Near to Meliata village, dark shales with radio-
larite, sandstone and olistostrome intercalations occur. Based
on radiolarians, the age of the radiolarite interbeds is Middle
Bathonian to Early Oxfordian (Kozur & Mock 1985; Kozur
et al. 1996). Large blocks (olistoliths) of Triassic rocks and
Triassic and Jurassic radiolarites commonly occur in the
shaly matrix. The olistostromes contain mostly carbonates of
a different composition. The lowermost olistostrome bed
contains 10—30 cm sized subangular clasts of Carnian grey
cherty limestone and 10—20 cm sized angular clasts of red
radiolarian chert. It is followed by calcareous shale contain-
ing an upward decreasing amount of Carnian and Norian
limestone blocks (Mock et al. 1998). It is overlain by spotty
Fig. 20. The encountered foraminiferal assemblage from the matrix of the calciturbidites in Csipkés Hill. 1 – Callorbis minor? Wernli &
Metzger. 2 – Nodosaria sp. 3 – Eoguttulina sp. and Trochammina sp. 4 – Protopeneroplis striata? Weynschenk. 5 – Planiinvoluta sp.
6 – Siphovalvulina? sp. 7 – Tubinella? sp. 8 – Valvulina sp. 9 – Trochammina sp.
376
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
shale with radiolarite interlayers and greyish green shales
with sandstone to microbreccia interlayers. In the coarser-
grained breccia metamorphosed limestone clasts are predom-
inant, but non-metamorphosed limestones of oomicrite and
oosparite texture also occur along with individual ooids and
oncoid grains and crinoid ossicles. In the finer-grained brec-
cia, the volcanic components (various kinds of submarine
basalts showing glass to “dolerite” texture – Mock et al.
1998) are dominant, but metamorphic carbonates and rarely
non-metamorphic oosparit are also present. Mn-bearing beds
are visible in the topmost part of the exposed section (Mock
et al. 1998).
The other important occurrence of the Meliata Unit is lo-
cated near to Jaklovce village. Here the melange is made up
mostly by olistoliths of various sizes whereas the sandstone
to microbreccia and olistostrome intercalations are less com-
mon in the Middle Jurassic dark shale matrix (Kozur &
Mock 1995). The blocks consist of light, probably shallow-
marine slightly metamorphosed limestones (Honce Limestone
of unknown age), siliciclastic rocks, pelagic cherty lime-
stones, dolomites, radiolarites, rhyolites, basalts, serpentinites.
In summary, the Meliata Unit in Slovakia is made up of
black and spotty shales with sandstone and olistostrome in-
tercalations. The main components of the olistostrome beds
are as follows: Anisian to Norian grey limestones, metamor-
phosed limestones, ooilitic limestones, red cherts, basalts of
backarc basin origin, rhyolites, and serpentinites. The sup-
posed age, the sedimentological features and the predomi-
nance of the Middle to Upper Triassic basin facies in the
carbonate components show a great similarity to the compo-
nents of the olistostrome beds of the TC in the Rudabánya
Hills. Moreover, the style of ductile deformation and the
temperature, pressure and age constraints of the low to very-
low grade metamorphism are very similar (Kövér et al.
2007). However, there are differences in the composition
and particularly in the proportion of the olistostrome compo-
nents. In the TC metamorphosed limestone clasts are rare,
the serpentinite clasts are missing and among the volcanic
components the rhyolite is predominant, while the basalt is
rare. In spite of the differences, the major similarities in the
sedimentation pattern and the later structural evolution may
indicate a common basin for the depositional area of these
units, in the vicinity of the ongoing nappe-stacking of the at-
tenuated continental margin and oceanic crust of the Neo-
tethys Ocean. The differences in the rate of clast composition
can be explained by deposition in other parts of the same ba-
sin, with variable distances from the distinct source areas.
Northern Calcareous Alps – Tirolic Nappe Group, Hall-
statt Mélange, Meliata
In the Northern Calcareous Alps various gravity mass flow
deposits occur in the Middle to Late Jurassic deep marine se-
quences reflecting closure of the Neotethys Ocean. In the
area of the Tirolic Nappe Group various basins of different
time range and sediment fill came into existence: Lammer
Basin (Callovian to Oxfordian), Tauglboden Basin (Oxford-
ian to Tithonian), Sillenkopf Basin (Kimmeridgian to Titho-
nian) (Gawlick et al. 1999, 2002; Gawlick & Frisch 2003).
From among these developments the Lammer Basin was
roughly coeval with the formation of the complexes studied
in the Rudabánya Hills.
The Lammer Basin received mass-flow deposits and large
slides derived from the grey Hallstatt facies zone (“Hallstatt
Mélange”). The thickness of the basin fill may reach 2000 m
(Gawlick 1996; Gawlick & Suzuki 1999). Cherty limestone
and marl basin facies and turbidites characterize the Callov-
ian. Olistostromes and large olistoliths originated from the
Pötschen Limestone occur in the Callovian to Lower Oxfor-
dian. The Middle Oxfordian is made up mostly by large slid-
ed blocks of the Lower Triassic Werfen Formation, Upper
Triassic Pötschen and reworked Hallstatt Limestone and
variation of olistostromes, marls and radiolarian cherts. The
upper part of the succession is composed of Middle and Up-
per Triassic platform carbonate mega-slides (Gawlick 2000).
The “Hallstatt Mélange” was defined as a complex that is
made up of reworked fragments of deposits formed on the
Late Triassic to Early Jurassic attenuated Neotethys margin,
and small remnants of the oceanic basement (Meliata Zone)
(Frisch & Gawlick 2003). It contains elements of the Zlam-
bach/Pötschen and Hallstatt Limestone and Meliata facies
zones, respectively. The “Hallstatt Mélange” was formed in
the late Early to early Late Jurassic interval as a result of a
successive shortening of the distal shelf area (Hallstatt
Zone). During this process trenches developed in the foreland
of the advancing nappes and filled up by various deposits, in-
corporated into the accretionary prism, subsequently. Parts of
the accretionary prism were resedimented in the Lammer Ba-
sin or occur as overthrusted remnants (e.g. the Florianikogel
Formation in the eastern Northern Calcareous Alps – Mandl
& Ondrejičková 1991, 1993; Kozur & Mostler 1992).
Remnants of the Meliata facies zone – representing the
most distal part of the shelf area and the continental slope, as
well as the transition to the Neotethys Ocean floor – are re-
ported from the eastern (Mandl & Ondrejičková 1991, 1993;
Kozur & Mostler 1992) and central part of the Northern Cal-
careous Alps (Gawlick 1993). These remnants occur partly
as metamorphosed, isolated slides (Florianikogel area) or as
clasts in olistostromes, consisting of Middle Triassic radi-
olarites and cherty marls, Carnian Halobia beds and Late
Carnian to Sevatian Hallstatt Limestone (Gawlick 1993).
The roughly coeval lower part of the Lammer Basin fill
shows some similarity in lithology (pelagic limestone and
radiolarite), sedimentary features and supposed geodynamic
position to that of the TC in the Rudabánya Hills. However,
there are remarkable differences in the clast composition of
the olistostromes. Those of the Lammer Basin consist only
of Middle to Upper Triassic pelagic limestone clasts, clasts
from the Lower Triassic Werfen beds, and bentonite, indicat-
ing a depositional area further from the arc.
Bükk—Darnó area – Mónosbél Unit
In the Bükk—Darnó area the Middle to Upper Jurassic
Mónosbél Complex – containing great amounts of gravity
mass flow deposits in shale and radiolarite matrix – is com-
parable to the contemporaneous formations in the Rudabá-
nya Hills.
377
LITHOFACIES AND AGE DATA OF JURASSIC SEDIMENTS (RUDABÁNYA HILLS, NE HUNGARY)
In the western part of the Bükk Mts, the Mónosbél Unit is
made up of Bajocian to Kimmeridgian deep marine siliciclas-
tics, carbonates and siliceous sediments with intercalations of
olistostrome beds, containing very heterogeneous clasts trans-
ported into the basin via gravity mass movements. In the olis-
tostrome beds, along with fragments of acidic, intermediate
and basic magmatites, phyllites, metasiltstones, metasand-
stones, pelagic carbonates and radiolarites, and lithoclasts of
redeposited carbonates – containing grains of shallow-water
origin (ooids, oncoids, and skeletal fragments of shallow ma-
rine biota) – are common. Large blocks (olistoliths and
blocks) of platform derived (“Bükkzsérc-type”) limestones of
Bajocian to Bathonian age are particularly common and typi-
cal in the Mónosbél Unit (Haas et al. 2006).
Gravity deposits of the Mónosbél Unit are also exposed in
the Darnó area and in ore exploratory wells at Recsk, Mátra
Mts. Olistoliths of marine Upper Permian and Upper Triassic
Hallstatt Limestone were encountered within Bajocian to
Callovian shale and radiolarite (Haas et al. 2006). The thick-
ness of the olistostrome-rich intervals may exceed 100 m.
The usually matrix supported breccia is typically oligomict,
consisting mostly of carbonate clasts of various colours and
compositions (Haas et al. 2006). Detailed component analy-
sis of the olistostromes is under way.
In a borehole drilled near Peak Kékes, Mátra Mts, Bajo-
cian platform derived redeposited carbonates, more proximal
than those in the Bükk Mts, were encountered in a remark-
able thickness (Haas et al. 2006).
In summary, the most characteristic features of this
Mónosbél Unit are the presence of coeval platform-derived
foraminifers, ooids, oncoids, peloids – redeposited as indi-
vidual clasts – and large amounts of Middle Jurassic shal-
low-water limestones of mm to tens of hundred m in size.
The individual clasts indicate that the source area of the plat-
form material must be a coeval, active carbonate platform,
most probably the Adriatic Carbonate Platform, which was the
only known Middle Jurassic active platform in the whole re-
gion (Tišljar et al. 2002; Vlahović et al. 2005). The presence
of rhyolite, andesite and basalt clasts are also common in
some horizons indicating the complexity of the provenance.
There is a common feature in the composition of the olis-
tostromes of the Mónosbél Unit and the TC, as well. The TC
contains some rhyolite and basalt, but the volcanic clasts
from the Mónosbél Unit are more varied.
Among the examined Jurassic series of the Rudabánya
Hills, the only one, which has Middle Jurassic platform de-
rived material, as a characteristic feature, is the Csipkés Hill
olistostrome. Like the Mónosbél Unit, it contains carbonate
turbidite beds with platform derived foraminifers (following
the previous reasoning: it probably originated from the Adri-
atic Carbonate Platform) and olistostrome horizons, but in
contrast to that, volcanites and roughly coeval lithoclasts are
missing among the clasts.
In the Dinarides ophiolite mélange complexes comparable
to those in the Bükk—Darnó area occur in the Dinaridic Ophio-
lite Belt (Dimitrijević et al. 2003). In the Dinaridic Ophiolite
Belt the ophiolite mélange contains fragments of obducted
ophiolites (lherzolite), Triassic and Jurassic limestone blocks,
and polymict olistostromes containing clasts of Middle Trias-
sic to Middle Jurassic radiolarian cherts, greywackes, basalts,
gabbros, ultramafic rocks, granites and Triassic and Jurassic
limestones in a Jurassic argillaceous, silty matrix (Karamata et
al. 2000; Pamić et al. 2002; Karamata 2006).
There are a lot of common sedimentological features in the
Middle to Upper Jurassic complexes discussed above that can
be attributed to the processes of the Neotethys closure. How-
ever, due to their different paleo-position, the composition of
the redeposited clasts shows significant differences depending
on geological features of the source area. Fragments originat-
ing from the Hallstatt facies zone occur in all of the compared
units. Grey Hallstatt-type limestones are typical components
of the Telekesoldal Complex; they are also characteristic ele-
ments of the lowermost olistostrome of the Meliata-type sec-
tion. Both grey and red Hallstatt-type pelagic carbonates
prevail in the Lammer and Sandlingalm Basin fill, and they
are present as olistoliths in the Mónosbél Complex of the
Darnó area. The clasts derived from the red Hallstatt-type area
are predominant in the olistostrome of Csipkés Hill.
Conclusions
Lithological and microfacies studies on the Jurassic sedi-
mentary rocks of the Aggtelek-Rudabánya led to the follow-
ing conclusions on the relationship, position, and age of the
different lithofacies units of the investigated complexes:
1. The Telekesvölgy Complex (TVC) is the sedimentary
cover of the Upper Triassic of the Bódva Series. The Norian
Hallstatt Limestone – well dated by conodonts – gets more
argillaceous upward and gradually progresses into reddish to
greenish and then grey marl that can be correlated to the latest
Triassic Zlambach Formation. Locally, it may contain slided
blocks of Middle to Upper Triassic hemipelagic limestones,
similar to those found in deeper stratigraphic levels of the
same succession. The variegated marl progresses into grey
marl and calcareous marl, containing significant amounts of
redeposited crinoid fragments. It may be interpreted as a hemi-
pelagic facies, relatively close to submarine highs. The upper-
most lithofacies unit of the TVC is black shale, rich in
radiolarians and sponge spicules. It is a typical deep pelagic
basin facies, Bajocian to Early Bathonian in age, according to
the revised radiolarian fauna.
2. The Telekesoldal Complex (TC) represents a mélange-
like subduction-related complex, composed of black shales,
sandstone turbidites and olistostrome horizons, deposited by
gravity mass flows. The most characteristic microfacies
types of the lowermost shale and marl lithofacies units are
radiolarian-sponge spicule wackestone and barren mudstone,
representing deep hemipelagic basin facies, akin to that of
the youngest lithofacies of the TVC. There are sandstone and
siltstone intercalations of turbiditic origin in the shale. The
sandstone-bearing shale lithofacies was formed in a relative-
ly deep pelagic basin that was reached by proximal to distal
siliciclasic turbidity currents. A relatively deep marine basin
in the proximity of a submarine slope is likely to be the dep-
ositional environment of the olistostrome lithofacies. The
components of the olistostromes are predominantly Middle
to Upper Triassic hemipelagic limestones rarely limestones
378
KÖVÉR, HAAS, OZSVÁRT, GÖRÖG, GÖTZ and JÓZSA
of platform facies, rhyolite and basalt. Bajocian—Callovian
age was proved from the complex by revising the radiolarian
data and finding the first marine palynomorphs in the Ag-
gtelek-Rudabánya Hills.
3. The Csipkés Hill olistostrome consists of carbonate tur-
bidite beds containing Jurassic platform-derived material
(including foraminifers) and olistostrome horizons contain-
ing limestone clasts of the Middle—Upper Triassic of red
Hallstatt facies. On the basis of the encountered foraminifer-
al assemblage, the Jurassic depositional age of these beds is
proven and a Middle Jurassic (Bajocian?) age is highly prob-
able. The platform derived individual foraminifers indicate a
coeval active carbonate platform in the neighbourhood of the
depositional basin.
Acknowledgments: The research was supported by the
Hungarian Scientific Research Found OTKA No. 48824,
61872, F048341. The authors are grateful to L. Fodor for
sample collection and structural investigations and to S.
Kovács for providing data on the previous examinations.
The thorough review by H.J. Gawlick is acknowledged.
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