GeolCarp_Vol57_No4_279

GEOLOGICA CARPATHICA, AUGUST 2006, 57, 4, 279—294

www.geologicacarpathica.sk

Sedimentology, paleoichnology and sequence stratigraphy of

a Karpatian sandy facies (Salgótarján Lignite Formation,

N Hungary)

ÁRPÁD DÁVID

, ZOLTÁN PÜSPÖKI

, PÉTER KÓNYA

, LÁSZLÓ VINCZE

, MIKLÓS KOZÁK

and RICHARD W. M

INTOSH

Károly Eszterházy College, Department of Geography, Leanyka út 6, 3300 Eger, Hungary; davida@ektf.hu

Debrecen University, Department of Mineralogy and Geology, Egyetem square 1, 4032 Debrecen, Hungary

Geological Institute of Hungary, Stefánia út. 14, 1143 Budapest, Hungary

(Manuscript received January 24, 2005; accepted in revised form December 8, 2005)

Abstract: Detailed sedimentological and paleoichnological investigations were done on the sandy facies of the sequence
stratigraphically well researched coal-bearing sediment series (Salgótarján Lignite Formation) in the East Borsod Basin
(Northern Hungary) to provide data for paleoenvironmental reconstruction. Collection and identification of bioerosional
and bioturbational reworked trace fossils were carried out within 9 stratigraphic levels of the outcrops representing 5
parasequences from the 25 of the entire series and reaching about 26 m in vertical extension. 11 sedimentological units
were dissected; 11 ichnogenera and 25 ichnospecies were identified and documented in the series. Regarding the
sedimentological data, the dominant facies zone of the sedimentation was the shoreface, mainly its upper and middle,
sometimes its lower part, while at the lower and/or uppermost parts of the parasequences some formations of fore- and
backshore and even lagoonal materials as well as open marine (offshore) sediments can appear. 4 ichnofacies, namely the
Entobia, Skolithos, Cruziana and Glossifungites were determined and described by paleoichnological and sedimento-
logical terms. Regarding these results in the framework of the sequence stratigraphic model, it can be concluded that in
the researched series the Entobia ichnofacies is related to the transgressive bars below the flooding surfaces of the
subsequent parasequence, Skolithos and Glossifungites ichnofacies are related to the foreshore, upper and middle
shoreface of the prograding parts of the parasequences while the Cruziana ichnofacies is related to the lower shoreface
of the prograding parts of the aggrading parasequences.

Key words: Karpatian, Hungary, sequence stratigraphy, paleoichnology.

Introduction and aims

In the last 5 years the sequence stratigraphic analysis of the
200—400 m thick coal-bearing Miocene Karpatian series in
Northern Hungary (Salgótarján Lignite Formation) was car-
ried out, one of the essential requirements of which was the
adequate description of its facies. The former paleoecologi-
cal reconstructions of the series (e.g. Báldi 1973; Bohn-Ha-
vas 1985; Korecz-Laky 1985) focused mainly on the silty
facies of lagoons and shallow marine environments. In order
to describe the bio- and lithofacies characteristics of the
sandy facies poor in fossils, sedimentological and paleoich-
nological investigations were made.

Sedimentological and paleoichnological investiga-

tions have been performed on well exposed outcrops
along the about 60 m high walls of a sand pit, which rep-
resents an important part of the whole series and was in-
terpreted in detail in the course of sequence-stratigraphic
research (Fig. 1).

The aims of this paper are:
– to identify the existing ichnofacies on the basis of a

joint documentation of the sedimentological and paleo-
ichnological data, and

– to determine the relationship between sequence

stratigraphic position and the contained ichnofacies of the

analysed sedimentary units giving their paleoenvironmen-
tal status.

Stratigraphic background

The Salgótarján Lignite Formation was formed during

the Karpatian Stage of the Miocene as a siliciclastic se-
ries of the TB2.2 (Haq et al. 1988) or Bur-4 (Vakarcs et
al. 1998) eustatic transgression with lagoonal (oligoha-
line) and shallow marine (polyhaline) silty intercalations
and with coal seams in the oligohaline facies (Püspöki
2002) (Fig. 2).

The series has a cyclic appearance, and as a result of se-

quence stratigraphic analysis we could detect 25 parase-
quences in the whole series. On the basis of the spatial
shifting of sedimentary circumstances, six important trans-
gressions and subsequent progradations can be separated
(Püspöki 2001) (Fig. 3). The series can be interpreted as a
transgressive and early highstand systems tract of one
eustatic 3

-order sequence. Within this sequence, four

-order cycles can be separated, three of which have

tectonic determination. The parasequences are 5

-order

cycles generated by the precession fluctuations. The series
has an aggrading character from the upper part of the 11

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DÁVID, PÜSPÖKI, KÓNYA, VINCZE, KOZÁK and M

INTOSH

parasequence to that of the 16

. The important influence of

small scale eustatic oscillations refers to the elevated mar-
ginal position of the sub-basin and to a relatively inten-
sive sedimentation, which can lead to the thickening of
the 5

-order cycles and to the occurrence of the oscillating

character. The coal beam V was formed by a retrogradation-
al period while the others (IV—I) were formed by prograda-
tional events, which is evidenced both by the facies pattern
of the enclosing sediment series and the geometry of the
coal beams like duplication, small horizontal extension in
the case of coal beam V (Püspöki 2001).

The series of the Csiga-Hill is exposed in four sand pits

and in a nearby road-cut (Fig. 1). The lithological column
correlated with the well log of the borehole Nb 98 and the

Fig. 1. Paleogeograpy and geographical position of Csiga Hill (Bánhorváti).

results of the material research are shown in Fig. 4. It is
well observable that the exposed series represents the 8

and 12

parasequences of the series. Unfortunately

the middle sand pit representing the 9

and 10

parase-

quences of the series, because of its poor conservation, is
not accessible now.

Methods

Sedimentological investigations were made partly in the

field with documentation of the stratification, and partly in
the laboratory as the determination of grain size distribu-
tion and the measurement of the carbonate content.

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SEDIMENTOLOGY, PALEOICHNOLOGY AND STRATIGRAPHY OF A KARPATIAN SANDY FACIES (HUNGARY)

Investigations of bioerosion were made on the material

of an Ostrea shell Bed by collection of bulk sample of
more than 200 Ostrea valves. The preservation of the col-
lected material was relatively poor (fragmented) and only
a certain portion was represented by complete Ostrea
valves, dominantly right, subdominantly left ones. Traces
of bioerosion were observed by stereomicroscope, identifi-
cation of them was made using ichnotaxonomical data by
Seilacher (1953, 1969), Boekschoten (1966, 1970), Bro-
mley (1970, 1992), Tasch (1973), Warme (1975), Bromley
& D’Alessandro (1983, 1984), Kelly & Bromley (1984),
Boucot (1990), Bromley & Martinell (1991), De Gibert et
al. (1998), Farinati & Zavala (2002). To recognize the in-
ner structure of the ichnospecies, epoxy casts were made
with ARALDIT AY 103 and HARTER HY 956 compo-
nents (Golubic et al. 1970). The preparation was carried
out at the laboratory of Károly Eszterházy College, De-
partment of Geography, Eger.

Observation of the bioturbation was carried out by large

scale (cm, dm, inch) mapping and in situ photo documen-
tation of the outcrops in the sand pits. The identifications
of the ichnospecies were made on photos, considering the
ichnotaxonomical data by Seilacher (1953, 1967), Crimes
& Harper (1970), Ekdale et al. (1984), Bromley (1990),
Bottjer & Doser (1992), Curran (1992), Ekdale (1992),
Maples & West (1992), de Gibert & Martinell (1995,
1999), Nielsen et al. (1996), Nara (1997, 2002). The ichno-
fabric index (ii) has been determined by using the classifi-
cation of Droser and Bottjer (Droser & Bottjer 1986).

Results

Sedimentological description of the series

The following description of the sedimentary units

(Fig. 4) is focused on the well preserved parts of the se-
ries suitable for detailed analysis.

Series of the lower sand pit

Small scale cross-stratified unit: The thickness is 2.4 m.

Moderately well sorted ( = 0.64—1.67) fine sand (mo-
de = 0.18 mm) and sandy fine pebbles with small scale rip-
ple lamination, and with some clayey silt along the bed
surfaces. Bioerosion cannot be seen, bioturbation is very
rare (ii 2).

Bioturbated unit: The thickness is 2.2 m. Moderately

sorted ( = 1.14) and poorly bedded sand, gravelly sand.
Bioerosion is lacking, bioturbation is strong (ii 3—4).

Lagoonal unit: The thickness is 1.3 m. Various beds of

poorly sorted silty sand, lagoonal clay, and clayey brown
coal. The overlying formation is a poorly preserved Ostrea
Bed with clayey matrix. Bioerosion can be seen on the
material of the Ostrea Bed (sponge and worm borings).

Ostrea Bed (poorly preserved): The thickness is 25—30 cm.

The Ostrea valves are mainly right ones, their size is not
more than 15 cm and lay on each other with their convex
side upwards, without any matrix. Bioturbation cannot

be seen, bioerosion is strong. The inner sides of the
valves are also bioturbated.

Laminated silt: Silty clay containing an association of

brackish foraminifers, the dominant species of which are
Rotalia beccarii and Nonion granosum.

Series of the Southern sand pit

Ostrea Bed (well preserved): The thickness is 30—50 cm.

The Ostrea valves are mainly left ones, their size is not
more than 15 cm and lay on each other with their convex
side upwards, without any matrix. Bioturbation cannot be
seen, bioerosion is strong.

Gravel bed with Ostrea valves: The thickness is 1.4 m.

Moderately sorted fine- and medium-sized gravel, gravel-
ly sand with slight bedding. Resedimented Ostrea valves
and driftwood fragments can also be seen. Both bioerosion
and bioturbation are characteristic.

Alternating laminated silt and sand: The thickness is 3.6 m.

Intercalations of thin layers of clayey silt and moderately sort-
ed ( = 1.074) medium-sized sand (mode = 0.142—0.277 mm).
Bioerosion is missing, but bioturbation is characteristic.

Large scale cross-stratified unit: The thickness is 4 m.

Moderately sorted ( = 0.919) medium-sized sand (mo-
de = 0.262—0.605 mm) with large scale cross-bedding and
with thin silt intercalations along the cross-laminae. The
thickness of beds is about 0.5 m. Bioerosion and bioturba-
tion cannot be seen.

Series of the wall of the road and the upper sand pit

Alternating laminated and cross-stratified unit: Moderate-

ly well sorted = 0.684) fine sand (mode = 0.074—0.095 mm).
The cross-bedding is variable in direction with varying an-
gles, and is locally replaced by laminar structures, some-
times with intercalations of clasts with clayey-silty
matrix (storm deposits). Bioerosion is missing, bioturba-
tion is significant.

Cyclic unit: This has a thickness of more than 10 m.

Rhythmic intercalations of moderately sorted sand (mo-
de = 0.042—0.114 mm,

= 1.13) and poorly sorted clayey

sandy silt (mode = 0.01—0.04, = 1.63). The surfaces of
the cycles are eroded. Bioerosion is missing, however
bioturbation is intensive. Ophiomorpha is the dominant
ichnogenus. It indicates lower shoreface within which
the material from the middle and upper shoreface had
also been transported during storms.

Trace fossil description

Inventory Numbers are related to the collection at the

Department of Geography Károly Eszterházy College,
Eger.

Bioerosion

Ichnogenus Entobia Bronn, 1838

Entobia cateniformis Bromley et D’Alessandro, 1984

(Fig. 5.1,2)

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SEDIMENTOLOGY, PALEOICHNOLOGY AND STRATIGRAPHY OF A KARPATIAN SANDY FACIES (HUNGARY)

S u b s t r a t e :

poorly preserved Ostrea valves from the

Ostrea Bed of the pit. The borings are stenomorphic. The
stenomorph character is indicated by the small diameter of
the apertures and the length of their canal. The chambers
are not as elongated as in the case of the idiomorphic
forms. Only the B growing phase occurred in the exam-
ined material. Collecting site: Ostrea Bed of the Southern
sand pit. Inv. Nos. E 25, E 28, E 75.

Entobia geometrica Bromley et D’Alessandro, 1984

(Fig. 5.3,4)

S u b s t r a t e :

poorly preserved Ostrea valves from the

Ostrea Bed of the pit. The forms are stenomorphic. This is
indicated by the relatively small diameter of the apertures,
by the shape of the apertural channels, by the small diame-
ter of the chambers and by the small number of the canal
connecting the chambers. Collecting site: Ostrea Bed of
the Southern sand pit. Inv. Nos. E 23, E 54.

Entobia laquea Bromley et D’Alessandro, 1984

S u b s t r a t e :

poorly preserved Ostrea valves from the

Ostrea Bed of the pit. Stenomorphic forms. Regarding the
shape of the chambers the spherical, slightly flattened forms
are dominant. The sizes of the apertures and chambers are
different from those of idiomorphic forms. Collecting site:
Ostrea Bed of the Southern sand pit. Inv. Nos. E 65.

Entobia megastoma (Fischer, 1868)

(Fig. 5.5)

S u b s t r a t e :

poorly preserved Ostrea valves from the

Ostrea Bed of the pit. Stenomorphic form. It is proved by
the number of the canals and by the lack of connection
between them. The diameters of the apertures also differ
from those of the idiomorphic forms. Collecting site: Ostrea
Bed of the Southern sand pit. Inv. Nos. E 27, E 30, E 32,
E 70.

Entobia paradoxa (Fischer, 1868)

(Fig. 5.6)

S u b s t r a t e :

also an Ostrea valve from the Ostrea Bed

of the pit. The apertures are relatively small; their diameter
is between 0.4 and 0.8 mm. Their shape is rounded. Aper-
tural canals are short. All of these canals are connected
with a chamber. The chambers form a one-level net and are
arranged more or less parallel to the surface of the sub-
strate. The sponge colony reached growing phase B. The
shape of the chambers is potato-like, elongated, amoe-
boid. Occurrence of thin apophyses is general. Collecting
site: Ostrea Bed of the Southern sand pit. Inv. Nos. E 24.

Entobia ovula Bromley et D’Alessandro, 1984

(Fig. 5.7)

S u b s t r a t e :

poorly preserved Ostrea valves from the

Ostrea Bed of the pit. It is a camerate entobian with round-

ed or oval apertures. The chambers are situated in large
numbers and are arranged close to each other. The cham-
bers are connected with extremely short canals. Character-
istic is the development of small barrel-like chambers. The
exploratory threads are slightly developed. Collecting site:
Ostrea Bed of the Southern sand pit. Inv. Nos. E 41, E 42.

Entobia isp. indet.

S u b s t r a t e :

poorly preserved Ostrea valve from the

Ostrea Bed of the pit. The character of the substratum in-
hibited the development of the idiomorphic form of the
bioerosion for this reason these cannot be identified at
ichnospecies level. Collecting site: Ostrea Bed of the
Southern sand pit. Inv. Nos. E 26.

Ichnogenus Caulostrepsis Clarke, 1908

Caulostrepsis taeniola Clarke, 1908

(Fig. 6.1)

S u b s t r a t e :

poorly preserved Ostrea valves from the

Ostrea Bed of the pit. The apertures are usually eight-
shaped. The gallery is cylindrical. Lengths vary between
3 mm and 7 mm. Smaller individuals are tongue-shaped
over the whole length, while the longer ones become thin-
ner at the vicinity of the aperture than at the distal end. In
most cases the structure lies within a plane. The surface is
smooth. Collecting site: Ostrea Bed of the Southern sand
pit. Inv. Nos. E 29, E 31, E 58, E 65, E 70.

Ichnogenus Maeandropolydora Voigt, 1965

Maeandropolydora decipiens Voigt, 1965

(Fig. 6.2)

S u b s t r a t e :

five Ostrea valves. Apertures are rounded.

The irregularly winding galleries are split. Width is between
0.8 and 1.1 mm. Length is around 1.5 cm. The most character-
istic feature of the ichnospecies are the pouches that can be
recognized clearly. Collecting site: Ostrea Bed of the South-
ern sand pit. Inv. Nos. Bh 6, Bh 47, Bh 54, Bh 101, Bh 171.

Maeandropolydora sulcans Voigt, 1965

(Fig. 6.3)

S u b s t r a t e :

seven Ostrea valves collected from the

Ostrea shelly Bed of the outcrop. The diameter of the
long, cylindrical galleries is between 0.8 and 1.2 mm.
They extend winding irregularly and forming loops of var-
ious sizes, which turn back and contact with themselves.
The galleries in the Ostrea valves in most instances imi-
tate the changes in the surface of the substrate. Collecting
site: Ostrea Bed of the Southern sand pit. Inv. Nos. Bh 15,
Bh 18, Bh 35, Bh 149, Bh 204, Bh 205, Bh 700.

Maeandropolydora elegans Bromley et D’Alessandro,

1984 (Fig. 6.4)

S u b s t r a t e :

eleven Ostrea valves collected from the

Ostrea shelly Bed of the outcrop. The tubes usually ex-

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tend over relatively great distances in pairs parallel with
each other. Irregular winding in different directions is
characteristic. Collecting site: Ostrea Bed of the Southern
sand pit. Inv. Nos. Bh 80, Bh 95, Bh 111, Bh 140, Bh 141,
Bh 142, Bh 145, Bh 334, Bh 544, Bh 601, Bh 804.

Ichnogenus Gastrochaenolites Leymeriere, 1842

Gastrochaenolites lapidicus Kelly et Bromley, 1984

(Fig. 7.1)

This is an elongated oval dwelling structure with

smooth surfaces. The cross-section is rounded all along
the tube except the immediate surroundings of the aper-
ture and at the base of the erosion where it may be oval.
The biggest diameter of a boring can be observed in the
equatorial region of the chamber. Collecting site: Ostrea
Bed of the Southern sand pit. Inv. Nos. E 29.

Gastrochaenolites cluniformis Kelly et Bromley, 1984

(Fig. 7.2)

This boring has a smooth surface. Along the main cham-

ber extend a primary incision opposite to which a less de-

Fig. 6. Trace fossils from the Csiga Hill sand pit. Bioerosion: 1 – Caulostrepsis taeniola Clarke, 1908 in inner side of left valve of Ostrea
sp. Collected at Csiga Hill middle sand pit. 2 – Maeandropolydora decipiens Voigt, 1965 in outer side of right valve of Ostrea sp. Col-
lected at Csiga Hill middle sand pit. 3 – Maeandropolydora sulcans Voigt, 1965 in outer side of right valve of Ostrea sp. Collected at Csi-
ga Hill middle sand pit. 4 – Maeandropolydora elegans Bromley et D‘Alessandro, 1983 in inner side of right valve of Ostrea sp.
Collected at Csiga Hill middle sand pit.

veloped secondary incision can also be observed at the
other side. The aperture and the neck are rounded or oval,
the base is cut in two. Collecting site: Ostrea Bed of the
Southern sand pit. Inv. Nos. E 70.

Gastrochaenolites torpedo Kelly et Bromley, 1984

(Fig. 7.3)

S u b s t r a t e :

two Ostrea valves. This is an elongated

smooth boring. The maximum diameter can be observed
in its middle part. The base is oval. The neck is com-
pressed but the aperture itself is oval nearly eight-shaped.
Collecting site: Ostrea Bed of the Southern sand pit. Inv.
Nos. Bh 800, Bh 805.

Gastrochaenolites turbinatus Kelly et Bromley, 1984

(Fig. 7.4)

S u b s t r a t e :

a single Ostrea valve. This is a cone-

shaped boring with smooth walls. Its widest part can be
observed near the rounded base. The cross-section is
rounded all along the boring. Collecting site: Ostrea Bed
of the Southern sand pit. Inv. No. Bh 310.

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SEDIMENTOLOGY, PALEOICHNOLOGY AND STRATIGRAPHY OF A KARPATIAN SANDY FACIES (HUNGARY)

Gastrochaenolites isp. indet.

(Fig. 7.5)

These are strongly eroded, poorly preserved borings.

Only a small part of the chambers can be observed. In most
cases even the species characteristics of the basal part can-
not be recognized. Collecting site: Ostrea Bed of the
Southern sand pit. Inv. Nos. Bh 141, Bh 157, Bh 164.

Ichnogenus Teredolites Leymeriere, 1842

Teredolites longissimus Kelly et Bromley, 1984

(Fig. 8.1)

The tubes are straight or slightly winding. They appear

in more consecutive levels as horizontal tube systems ly-
ing parallel to each other and to the surface of the substra-
tum, which is formed by a drift wood fragment. The
ichnospecies appears in the lower level of the southern pit
in the Ostrea valve bearing gravel bed in an embedded
one meter long driftwood fragment. The diameter of the
tubes is between 5 and 12 mm. Collecting site: Gravel bed
with Ostrea valves (Southern sand pit).

Ichnogenus Centrichnus Bromley et Martinell, 1991

Centrichnus concentricus Bromley et Martinell, 1991

(Fig. 8.2)

S u b s t r a t e :

eight Ostrea valves collected from the Os-

trea shelly Bed of the outcrop. This etching scar is a round-
ed hollow surrounded by a flat margin slightly eroded into
the substratum. The outline of the margin is oval, scalloped
and frequently ornamented by concentric rings. Collecting
site: Ostrea Bed of the Southern sand pit. Inv. Nos. Bh 59,
Bh 104, Bh 124, Bh 125, Bh 126, Bh 401, Bh 402, Bh 403.

Bioturbation

Collecting sites are determined by the stratigraphic no-

menclature given in the sedimentological description of
the series and on Fig. 4.

Ichnogenus Skolithos Haldeman, 1840

Skolithos linearis Haldeman, 1840

(Fig. 9.1,2)

Fig. 7. Trace fossils from the Csiga Hill sand pit. Bioero-
sion: 1 – Natural cast of Gastrochaenolites lapidicus Kelly et
Bromley, 1984 in right valve of Ostrea sp. Collected at Csiga
Hill middle sand pit. 2 – Gastrochaenolites cluniformis Kelly
et Bromley, 1984 in right valve of Ostrea sp. Collected at Csi-
ga Hill middle sand pit. 3 – Gastrochaenolites torpedo Kelly et Bromley, 1984 in right valve of Ostrea sp. Collected at Csiga Hill mid-
dle sand pit. 4 – Natural cast of Gastrochaenolites turbinatus Kelly et Bromley, 1984 in right valve of Ostrea sp. Collected at Csiga Hill
middle sand pit. 5 – Cross-section of Gastrochaenolites isp. indet. in right valve of Ostrea sp. Collected at Csiga Hill middle sand pit.

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Skolithos linearis is a simple straight burrow with much

larger length than width. The burrow is always perpendicu-
lar to the surface of the layer. Its diameter is not more than a
few mm. In the outcrop it appears in great numbers in the
laminated sand-mud series. Collecting site: Alternating
laminated silt and sand (Southern sand pit), alternating
laminated and cross-stratified unit of the wall of the road.

Ichnogenus Rosselia Dahmer, 1937

Rosselia socialis Dahmer, 1937

(Fig. 9.3,4)

A cone-shaped cave with a vertical tube in the substra-

tum the depth of which is several centimeters. It has a cen-
tral, usually vertical tube surrounded by structures
containing concentric laminae. The shape of these struc-
tures can vary from bulbous to cone-shaped. The tube nar-
rows with depth. The dwelling place was formed by the
sessile animal moving upward in the cave simultaneously
with sedimentation. Diameter may be 2—10 cm, length can
reach 50 cm. In horizontal cross-section the central sandy
tubes appear surrounded by concentric clayey laminae.
Collecting site: Alternating laminated and cross-strati-
fied unit of the upper sand pit (Northern end).

Ichnogenus Planolites Nicholson, 1873

Planolites isp.

(Fig. 9.5)

Irregularly sinuous slightly inclined unbranched bur-

row; 0.8—1.1 cm in diameter. It is preserved in full relief at
the locality. The ichnotaxon also occurs in the gravel lay-
er of the lower sand pit and at the thin bedded clayey-
sandy profile of the middle sand pit of the southern part of
the exposure. Collecting site: Gravel bed with Ostrea
valves, alternating laminated silt and sand (Southern
sand pit).

Ichnogenus Ophiomorpha Lundgren, 1891

Ophiomorpha nodosa Lundgren, 1891

(Fig. 10.1,2)

Apertures were not observable in the bedding planes of

the pit since they are narrow and lack encrusting nodules
so the chance of fossilization is rather small. The apertures
usually extend in vertical shafts but fossil examples of this
cannot be observed either. However, great numbers of sim-
ple, T- or Y-shaped branching tubes can be seen in both
cross- and in longitudinal section. Collecting site: upper
bed in the bioturbated unit of the lower sand pit, alternat-
ing laminated and cross-stratified unit of the upper sand
pit (Northern end).

Ophiomorpha isp.

(Fig. 10.3—5)

The traces cannot be determined on ichnospecies level

because the apertures are not exposed in the examined
beds. However the vertical shafts can be observed in the

lower part of the southern pit in the sandy pebble and can
be seen in great numbers in the laminated sand-mud series.
These shafts are only a few cm in length and the connect-
ed tubes are missing. Since the beds are rather thin the or-
ganisms were not be able to form a branching tube system
in the deeper parts. In thicker beds vertical cavities also
appear. In the laminated sandy-muddy series of the pit the
ichnospecies can be observed frequently together with
Skolithos linearis. Collecting site: Alternating laminated
silt and sand (Southern sand pit).

Ichnogenus Thalassinoides Ehrenberg, 1944

Thalassinoides suevicus (Rieth, 1932)

(Fig. 11.1)

This trace fossil is a burrow network with smooth walls.

The apertures extend into vertical shafts. These shafts are
connected by horizontal or inclined tubes. Between the
shafts and tubes or between the tubes there are Y- (120º) or
T- (90º) shaped connections. Y-shaped connections are the
most characteristic for the ichnospecies. The branching
and anastomosing tubes form a labyrinth in one or more
planes while the numerous connected shafts and tubes
form a three-dimensional net. Labyrinths are more fre-
quent than nets. Apertures and connecting vertical shafts
are not visible in the outcrop but the Y-shaped branching
points and the inclining orientation of the tubes can be
observed well. Collecting site in the outcrop: Alternating
laminated silt and sand (Southern sand pit).

Thalassinoides isp. (Fig. 11.2—6)

Cross-sections with irregular shape can also be ob-

served. These might have been dwelling places and were
formed by repeated usage. It is not common that the tubes
intersect in the same plane. However, both vertical cavi-
ties and connecting tubes can appear in deeper beds. It is
well observable in the figure that at the dual Y-shape
branching point a horizontal tube also appears. It also can
be found that an inclined tube turns back and then spreads
horizontally. The small ramifications (“appendices”) are
common in both the vertical and horizontal tubes. Some-
times the tubes are arched at the cavity system of the trace
fossil. Collecting site: lower bed in the bioturbated unit of
the lower sand pit, alternating laminated silt and sand
(Southern sand pit).

The ichnofacies

In the following we list the ichnofacies identified de-

scribing the enclosing lithofacies, determining the enclos-
ing sedimentary unit, giving the list of ichnotaxa and a
short description of the bioerosion or bioturbation.

Entobia Ichnofacies (sensu Bromley & Asgaard 1993)

L i t h o f a c i e s :

Strongly cemented Ostrea shelly Bed

containing variable but mostly only a small amount of

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matrix. The Ostrea valves are reworked and strongly frag-
mented, with upwardly convex orientation. The majority
(59.5 %) of the shell remnants are left valves.

P o s i t i o n :

The Ostrea Bed of the southern sand pit.

I c h n o t a x a :

Entobia cateniformis, Entobia geometri-

ca,  Entobia laquea,  Entobia megastoma,  Entobia para-
doxa,  Entobia ovula,  Entobia isp. indet., Caulostrepsis
taeniola,  Maeandropolydora decipiens,  Maeandropolydo-
ra sulcans,  Maeandropolydora elegans,  Gastrochaenolites
lapidicus,  Gastrochaenolites cluniformis,  Gastrochaeno-
lites torpedo,  Gastrochaenolites turbinatus,  Gastrochaen-
olites isp. indet., Centrichnus concentricus.

The series is a good example for Entobia ichnofacies

(Bromley & Asgaard 1993).

B i o e r o s i o n :

The Ostrea valves are moderately bio-

eroded. The shallow borings occur maily in the surface of
the valves. The diversity of the bioerosional traces is great.
The traces are well preserved, but in the case of common
presence of several ichnogenera identification of the ichno-
species was difficult.

Skolithos Ichnofacies (sensu Seilacher 1967;

Pemberton et al. 1992)

L i t h o f a c i e s :

Poorly bedded and poorly sorted pebbly

sand. The bed surfaces are strongly eroded by bioturbation.

Changing series of clayey silt and silty sand. The thick-

ness of the bed is 1—10 cm, the bed surfaces are undulat-

Fig. 10. Trace fossils from the Csiga Hill sand pit.
Bioturbation: 1 – Ophiomorpha nodosa Lundgren,
1891 in fine-grained sandstone. Locality: Csiga Hill,
lower sand pit. 2 – Ophiomorpha nodosa Lundgren,
1891 in fine-grained sandstone. Locality: Csiga Hill,
northern end of the upper sand pit. 3 – Ophiomorpha
isp. in an eroded bed surface. Locality: Csiga Hill, northern end of the upper sand pit. 4 – Ophiomorpha isp. in fine-grained sandstone.
Locality: Csiga Hill, northern end of the upper sand pit. 5 – Ophiomorpha isp. in clayey sandstone. Locality: Csiga Hill, southern sand pit.

291

SEDIMENTOLOGY, PALEOICHNOLOGY AND STRATIGRAPHY OF A KARPATIAN SANDY FACIES (HUNGARY)

Fig. 11. Trace fossils from the Csiga Hill sand pit. Bioturbation: 1 – Thalassinoides suevicus Rieth, 1932 in clayey sandstone. Locality:
Csiga Hill, southern sand pit. 2 – Thalassinoides isp. in sandstone. Locality: Csiga Hill, lower sand pit. 3 – Thalassinoides isp. in sand-
stone. Locality: Csiga Hill, lower sand pit. 4 – Thalassinoides isp. in sandstone. Locality: Csiga Hill lower sand pit. 5 – Thalassinoides
isp. in sandstone. Locality: Csiga Hill lower sand pit. 6 – Thalassinoides isp. in sandstone. Locality: Csiga Hill lower sand pit.

ing. The sand is moderately sorted, sometimes it may be
reworked even by wind under dry conditions.

P o s i t i o n :

The bioturbated unit of the lower sand pit,

the alternating laminated silt and sand in the southern
sand pit, alternating laminated and cross-stratified unit in
the wall of the road.

I c h n o t a x a : Ophiomorpha

isp., Skolithos linearis.

B i o t u r b a t i o n :

The rate of bioturbation is high, while

its diversity is low (ii 3—4). The different ichnospecies oc-
cur together. The complex evolution of the burrows of
Ophiomorpha isp. and Planolites isp. was inhibited by
thin character of the enclosing beds. The preservation of
the burrows is worse so they could be identified only at
ichnogenus level. Because of the relatively strong pale-

ocurrents the bed surfaces were commonly erosionally de-
creased, so the entrance of the burrows could not be pre-
served. The lumens of the burrows formed in the pebbly
sand are filled with the finer material of the overlying strata.

Cruziana Ichnofacies (sensu Seilacher 1967;

Pemberton et al. 1992)

L i t h o f a c i e s :

Moderately sorted, cross-layered or

laminated fine sand. Bed surfaces are frequently eroded,
locally with small clasts of clayey silt material along the
bed surfaces (storm deposits).

P o s i t i o n :

Cyclic unit in the upper sand pit.

I c h n o t a x a :

Planolites isp., Rosselia socialis.

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INTOSH

B i o t u r b a t i o n :

Planolites isp. is relatively rare and

because of its poor preservation it cannot be identified at
ichnospecies level. Rosselia socialis is relatively com-
mon in the given strata and because of its good preserva-
tion the morphological characteristics (vertical shafts,
cone like structures) are clearly observable, but having
been prepared by natural erosional processes the vertical
tubes connecting the cone like caves can easily be de-
stroyed (ii 3).

Glossifungites Ichnofacies (sensu Seilacher 1967;

Pemberton et al. 1992)

L i t h o f a c i e s :

Slightly stratified, poorly sorted sand

with strongly bioturbated bed surfaces, occasionally with
convolute forms.

P o s i t i o n :

Bioturbated unit in the lower sand pit.

I c h n o t a x a : Thalassinoides suevicus,

Thalassinoides isp.

B i o t u r b a t i o n :

The burrows form a complex net in

the exposed strata. The preservation is very good, the mor-
phological characteristics (T- and Y-form junctions) are
clearly observable, so the ichnospecies can be easily
identified (ii 4). The lumens of the burrows are filled with
pebbly sand of the overlying bed.

Discussion – Sequence stratigraphic position and

paleoenvironments of the sedimentary units and

the enclosed ichnofacies

In the paleoenvironmental evaluation of the outcrop we

had to consider, that a parasequence follows Walter’s law,
while at the boundary of parasequences a gap in the facies
can appear. From this point of view, referring to the gener-
alized model and facies zones of a siliciclastic shallow
marine shore zone (Fig. 12) the sediment series of the Csi-
ga Hill can be interpreted well mostly in good accordance
with the sequence stratigraphic model of the series some-
times giving additional data on undecided questions. In
the order of the stratigraphic position we can reconstruct
the following paleoenvironments (Fig. 4):

– The lower sand pit represents the upper prograding part

of parasequence 8, and the flooding surface of parasequence

9. An upper shoreface is represented by the lower small scale
cross-stratified unit without significant bioturbation and by
the bioturbated unit, where the identified ichnofacies are
Glossifungites and Skolithos. The end of progradation is rep-
resented by the appearance of the coal-bearing lagoonal
unit, while along and above the flooding surface of the next
parasequence the Ostrea Bed of the transgressive bar with
sponge borings and the laminated silt of the offshore envi-
ronments with foraminifers was accumulated.

– The Southern sand pit represents the uppermost beds

of parasequence 10 and the flooding surface and earlier
part of parasequence 11. The Ostrea Bed with a well pre-
served  Entobia  ichnofaces represents a transgressive bar
while the gravel bed with Ostrea valves with driftwood
fragments with Teredolites longissimus specimens is the
material of a short-term gravelly back shore paleoenviron-
ment. The flooding surface of parasequence 11 starts with
the  alternating laminated silt and sand with well pre-
served  Skolithos  and  Cruziana  ichnofacies representing
the intertidal swash zone of a foreshore with a depth of
about 4 m. The upper part of the Southern sand pit with
the  large scale cross-stratified unit and without any bio-
turbation represents the upper part of parasequence 11 re-
flecting longshore bars of the middle shoreface.

– From the upper part of parasequence 11 to parase-

quence 16 the series has an aggrading character (Fig. 3)
where significant facies shifting cannot be detected in
the zone of the Csiga Hill, so the dissection of the parase-
quences is uncertain and instead of the trend like shift-
ing of facies from offshore to backshore, a permanent
existence of the shoreface with slight change from the
upper to the lower part can be observed. The first stage of
this is the above mentioned longshore bar series of the
Southern sand pit. The next stage is the alternating lami-
nated and cross-stratified unit of the wall of the road and
of the upper sand pit with Cruziana and Skolithos ichno-
facies which also reflect a middle shoreface. The latter is
followed by the cyclic unit containing Ophiomorpha
specimens, which represents the appearance of the lower
part of the shoreface with cycles reflecting storm events
within the flooding period of parasequence 12. Consid-
ering the last statement the parasequence boundary be-
tween parasequences 11 and 12 needs some correction

Fig. 12. Facies zones and paleoenvironments of a siliciclastic shallow marine shore zone.

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SEDIMENTOLOGY, PALEOICHNOLOGY AND STRATIGRAPHY OF A KARPATIAN SANDY FACIES (HUNGARY)

from the depth of 51.6 m to 57.2 m in the borehole Nb 98
(see on Fig. 4).

Conclusions

Entobia, Skolithos, Cruziana and Glossifungites ichno-

facies were determined and described by the lithofacies,
ichnotaxa and by the characteristics of the bioerosion and
bioturbation.

Regarding the sedimentological data, the dominant fa-

cies zone of the sedimentation was the shoreface, mainly
its upper and middle, sometimes its lower part, while at the
lower and/or uppermost parts of the parasequences some
formations of fore- and backshore and even the lagoonal
materials can appear just as sediments of open marine (off-
shore) sediments.

Compiling the sedimentological and ichnofacies data

with the sequence stratigraphic model we can state that in
the researched Karpatian series (Fig. 4):

– Entobia Ichnofacies is related to the transgressive bars

below the flooding surfaces of the subsequent parasequence;

– Skolithos and Glossifungites Ichnofacies are related

to the foreshore, upper and middle shoreface of the pro-
grading parts of the parasequences;

– Cruziana Ichnofacies is related to the lower shore-

face of the prograding parts of aggrading parasequences.

With the necessary correction of the boundary between

the 11

and 12

parasequences, the research gives a good

example for drawing a conclusion on sequence strati-
graphic boundaries defined in well logs in accordance
with paleoichnological and sedimentological data.

Acknowledgments:

We extend our special thanks to Ri-

chard G. Bromley (Copenhagen) for his critical comments
and improvement of the English text. Special thanks to
Jordi M. de Gibert (Barcelona), Jozef Michalík (Bratisla-
va) and Radek Mikuláš (Prague) who were the official re-
viewers of the manuscript.

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