GeolCarp_Vol63_No2_107

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, APRIL 2012, 63, 2, 107—120 doi: 10.2478/v10096-012-0009-3

Introduction

Most of ichnological studies on flysch deposits concern thin-
and medium-bedded turbiditic sediments, in which the diver-
sity of trace fossil is generally high. Less attention is paid to
shaly flysch (e.g. Mikuláš et al. 2009) or thick-bedded sand-
stone-dominated  deep-sea  deposits  (e.g.  Heard  &  Pickering
2008; Phillips et al. 2011), mostly because they are less at-
tractive due to their general low trace fossil diversity, and of-
ten in the Carpathians due to their poor exposure, except for
quarries.  However,  it  is  expected  that  such  deposits  with
sand-dominated substrate represent a specific paleoenviron-
ment  for  burrowing  organisms,  which  needs  closer  charac-
terization,  because  most  flysch  trace  fossils  represent
mud-dwellers adapted to muddy substrates (Kern 1980).

The Lower Istebna Beds (Campanian—Maastrichtian) is a

peculiar  Late  Cretaceous  lithostratigraphic  unit  of  the
Silesian  Nappe  in  the  Flysch  Carpathians,  which  occupies
large  areas  and  is  dominated  by  thick-bedded  sandstones
(e.g. Unrug 1963, 1968). The sandstones have been quarried
for a long time as a building stone and the quarries together
with some natural outcrops give an opportunity to study their
trace fossils and ichnofabrics.

The aim of this paper is to present and interpret trace fos-

sils and ichnofabrics of the Lower Istebna Beds in selected
outcrops (Figs. 1—7), mainly in the middle sector of the
Polish part of the Silesian Nappe. The collected and illustrated
specimens (collection prefix INGUJ181P) are housed in the
Institute of Geological Sciences of the Jagiellonian University
in Cracow.

The Lower Istebna Beds have not been ichnologically in-

vestigated in detail. The occurrence of Spirorhaphe and

Ichnology of Upper Cretaceous deep-sea thick-bedded flysch

sandstones: Lower Istebna Beds, Silesian Unit

(Outer Carpathians, southern Poland)

JACEK RAJCHEL

and ALFRED UCHMAN

AGH – University of Sciences and Technology, Faculty of Geology, Geophysics and Environment Protection, Department of General

Geology, Environment Protection and Geotourism, al. A. Mickiewicza 30, 30-059 Kraków, Poland; jrajchel@geol.agh.edu.pl

Institute of Geological Sciences, Jagiellonian University, Oleandry Str. 2a, 30-063 Kraków, Poland; alfred.uchman@uj.edu.pl

(Manuscript received May 19, 2011; accepted in revised form September 30, 2011)

Abstract: The Ophiomorpha rudis ichnosubfacies of the Nereites ichnofacies was recognized in thick- and very thick-
bedded sandstones of the Lower Istebna Beds (Campanian—Maastrichtian), which were deposited mainly in deep-sea
clastic ramps and aprons. It contains mainly Ophiomorpha rudis (produced by deeply burrowing decapod crustaceans)
and rarely Zoophycos isp. and Chondrites isp. The impoverished Paleodictyon ichnosubfacies of the Nereites ichnofacies
is present in the medium- and thin-bedded packages of flysch sandwiched between the thick- and very thick-bedded
sandstones. They contain Chondrites isp., Phycosiphon incertum, Planolites isp., Arthrophycus strictus, Thalassinoides
isp., Ophiomorpha annulata, O. rudis, Scolicia strozzii and Helminthorhaphe flexuosa. The relatively low diversity of
this assemblage is influenced by limited areas covered by muddy substrate, which favours deep-sea tracemakers, and
partly by a lowered oxygenation in the sediment.

Key words: Upper Cretaceous, Polish Carpathians, Silesian Nappe, flysch, trace fossils, Ophiomorpha rudis.

Cosmorhaphe  was  mentioned  by  Unrug  (1963),  who  also
noted  vertical  burrows  that  pass  downward  into  horizontal
systems  on  the  soles  of  thick  beds,  which  are  described  as
Ophiomorpha  rudis  in  this  paper.  Książkiewicz  (1968)  de-
scribed Gyrophyllites, mentioned occurrence of a few types of
trace fossils (Książkiewicz 1975) and noted sixteen ichnotaxa
in  eleven  outcrops  (Książkiewicz  1977)  (Table 1),  indicating
that this is one of the poorest lithostratigraphic unit in the Polish
Carpathians  concerning  trace  fossils.  Rajchel  &  Uchman
(2008) presented ichnology of the Łęki section, and Rajchel &
Uchman (2009) described Ophiomorpha rudis from the Lower
Istebna Beds building stones in the architecture of Cracow.

Geological setting

The Istebna Beds, distinguished by Hohenegger (1861),

were split (Liebus & Uhlig 1902) into the Lower Istebna Beds
(thick-bedded  sandstones  and  conglomerates)  and  the  Upper
Istebna  Beds  (thick-bedded  sandstones  and  conglomerates,
dark  shales  with  sideritic  concretions,  black  mudstones  with
exotic  blocks).  In  the  eastern  part  of  the  Polish  Carpathians
(Krosno  region),  the  Upper  Istebna  Beds  are  distinguished
(Zuber  1915)  as  the  Czarnorzeki  Beds  (see  also  Świdziński
1947). In the Beskid Śląski range (western part of the Polish
Carpathians),  where  the  Istebna  Beds  are  thickest  (at  least
1600 m), and also in other areas, they are subdivided into the
Lower  Istebna  Beds  (thick-bedded  conglomerates  and  sand-
stones, pebble mudstones, packages of thin-bedded calcareous
sandstones  and  shales)  and  the  Upper  Istebna  Beds  (mostly
dark non-calcareous shales of the Lower Istebna Shale, mostly
thick-bedded  sandstones  and  debris-flow  deposits  of  the

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Upper Istebna Sandstone, mostly dark non-calcareous shales
of the Paleocene Upper Istebna Shale; Unrug 1968; Fig. 2).
Strzeboński (2001) included the Lower Istebna Shale in the
Lower Istebna Beds, which are not considered in this paper.

The Lower Istebna Beds (Campanian—Maastrichtian) are

composed  mostly  of  thick-  and  very  thick-bedded,  mainly
medium-  to  coarse-grained,  locally  conglomeratic  sand-
stones, which occupy large areas of the Silesian Nappe (Unrug
1963, 1968; Bromowicz et al. 1976). In the study area, they
are  developed  as  700—800 m  thick  (Leśniak  &  Słomka
2000),  mostly  poorly  sorted  oligomictic  quartz  arenites,  ar-
koses or greywackes (Kamieński et al. 1967; Bromowicz et

al. 1976; Bromowicz 2001), which are dirty white with rusty
spots, pale yellow, rusty cream or brownish in colour. The
sandstones are highly porous, weakly cemented by clay min-
erals, locally with silica. Stronger, concretionary carbonate
cementation is present in some beds. Thickness of the beds
attains 5 m or rarely even more. Many beds are amalgamated
and display an erosive, commonly channelized base.

The thick-bedded sandstones can be ascribed to a few

lithofacies  determined  as  sandy  conglomerates,  sandstones
and  sandstones  with  mudstones,  rarely  to  sedimentary  de-
formed  deposits  (Strzeboński  2003).  They  originated  from
non-turbulent  gravitational  flows,  sandy-debris  or  turbiditic

Fig. 1. Geological sketch map of the Polish Carpathians (based on Żytko et al. 1989; changed, simplified) with indication of the study areas.
A—D refers to the maps in Fig. 3. Numbers in circles refer to the localities in Table 1.

Table 1: Published data on occurrence of trace fossils in the Lower Istebna Beds (compiled from Książkiewicz 1977). Original names in
quadrangle parentheses; revised names by Uchman (1998). Localities: 1 – Będzieszyna, 2 – Czchów (in a package of the “Inoceramian
type flysch”), 3 – Czarnorzeki, 4 – Istebna, 5 – Istebna – river Olza, 6 – Kobyle n. Jasło, 7 – Łapanów, 8 – Łazy, 9 – Rożnów,
10 – Tabaszowa, 11 – Wiśnicz. The localities are indicated in Fig. 1 (numbers in circles).

Ichnotaxa\outcrops

1 2 3 4 5 6 7 8 9 10 11

Ophiomorpha annulata (Książkiewicz) [Sabularia simplex Książkiewicz]

Ophiomorpha rudis (Książkiewicz) [*Sabularia rudis Książkiewicz]

x x x x

Chondrites intricatus (Brongniart) [Chondrites aequalis Sternberg]

Chondrites targionii (Brongniart [Chondrites affinis (Brongniart), Chondrites arbuscula Fischer-Ooster,
Chondrites furcatus (Brongniart)]

Cladichnus fisheri D’Alessandro & Bromley [Taenidium isseli (Squinabol)]

Scolicia strozzii (Savi & Meneghini) [Taphrhelminthopsis auricularis Sacco]

?Scolicia prisca de Quatrefages [Scolicia vertebralis Książkiewicz]

Helminthorhaphe isp. [Helminthoida crassa Schafhäutl]

x x

Gyrophyllites rehsteineri Fischer-Ooster [Gyrophylithes kwassizensis Glocker]

x x x x

Spirophycus bicornis (Heer)

Cardioichnus isp. [Pararusophycus oblongus Książkiewicz]

Spirorhaphe involuta (De

Strefani)

Lorenzinia kuzniari Książkiewicz

Paleodictyon strozzii Meneghini [Paleodictyon tellini Sacco]

Paleodictyon miocenicum Sacco

cf. Beaconites caprinus Frey & Howard [Keckia hoessi Sternberg)]

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flows  (for  origin  of  such  deposits  see  Shanmugam  2000).
The  pebble  mudstones  were  deposited  as  cohesive  debrites
(Strzeboński 2005). A transition from debris flow to turbiditic
sandstones  has  been  observed  in  some  thick  and  very  thick
beds  (Felix  et  al.  2009).  The  deposits  of  the  Lower  Istebna
Beds can be ascribed mainly to the channel (Stanley & Unrug
1972)  and  overchannel,  rarely  depositional  lobe  facies  in
terms of the classical fan system (e.g. Mutti & Ricci Lucchi
1972; Walker 1978). However, lately, they are referred to a
siliciclastic ramp or apron (Stow et al. 1996), that has been

fed from multiple-points in proximity to their clastic material
source  (Strzeboński  2003).  The  source  was  situated  on  the
Silesian Ridge (the so-called Silesian Cordillera) rimming the
Silesian  Basin  from  the  south  (Książkiewicz  1962;  Unrug
1963, 1968; Strzeboński 2003). Taking in account several mil-
lion  years  lasting  sedimentation  of  the  Lower  Istebna  Beds,
activity of the source can be referred rather to a tectonic acti-
vation of the Silesian Ridge than to a eustatic sea-level fall.

Thin- and medium-bedded, non-calcareous flysch occurs

as packages between the dominating thicker beds (Fig. 8B),
usually  with  gradual  transition  from  thick-bedded  packages
at  the  base  (Wola  Komborska  quarry;  Fig. 6)  or  vice  versa
(Czasław 2 quarry; Fig. 5). Moreover, rare packages of gen-
erally calcareous thin- and medium-bedded flysch are sand-
wiched  between  thick-bedded  non-calcareous  sandstones
(Łęki-river section; Fig. 7). They are called the “Inoceramian-
type  flysch”  in  the  Istebna  Beds  (Skoczylas-Ciszewska  &
Kamieński 1959). Such sediments contain grey, mostly fine-
grained, horizontally and/or ripple laminated sandstones and
dark  grey,  light  grey,  greenish-grey  and  greenish  spotty
mudstones.  The  non-calcareous  greenish-grey  and  greenish
mudstones are locally present also between some non-calcar-
eous  thick-bedded  sandstones.  Judging  from  the  generally
non-calcareous  background  shales,  the  Lower  Istebna  Beds
were  deposited  below  the  calcium  compensation  depth
(CCD) (Koszarski & Żytko 1965; Książkiewicz 1975; Geroch
& Koszarski 1988), probably at the depth of 3500 m (Słomka
et  al.  2006)  or  at  least  4000 m  (Uchman  et  al.  2006).  They
contain  the  flysch-type  agglutinated  foraminifers  (Olszewska
& Malata 2006), which are typical of the bathyal and abyssal
zones below the CCD (Gradstein & Berggren 1981).

Studied sections

The Lower Istebna Beds were studied at Łęki near Trze-

meśnia in a quarry and natural outcrops (Łęki-klippe and
Łęki-river sections) and in the quarries at Czasław (Czasław 1
and 2) near Dobczyce, at Sobolów, Zonia and Leksandrowa in
the Bochnia region, and at Wola Komborska near Krosno
(Fig. 1).

The section at Łęki (Figs. 1, 3A), 112 m thick, starts in a

quarry (GPS coordinates: N49°49.906

’; E020°01.296’; ±6 m;

Fig. 4); it continues in the right bank of the Trzemeśnianka
River (Łęki-river section; thin-bedded flysch; Fig.7) and in a
steep klippe near the bridge (GPS coordinates: N49°49.915

’;

E020°01.270

’; ±6 m; Fig. 4) (Bromowicz 2001; Rajchel &

Uchman 2008). The beds are inclined to the north in the south-
ern limb of the Bulinka-Osieczany Syncline (Burtan 1984). In
the quarry and in the klippe, the sandstones are thick- and very
thick-bedded, medium-grained, poorly sorted, conglomeratic at
the base of some beds, commonly amalgamated, massive or ex-
ceptionally  large  scale  cross-laminated  in  the  lower  part  or  in
the whole bed. They contain irregularly-distributed intraclasts,
armoured (Fig. 8E) and non-armoured mudballs, which are up
to more than a meter in diameter. Locally, the mudballs are dis-
tributed  along  the  amalgamation  surfaces,  particularly  within
the  thickest  sandstone  beds.  Some  larger  intraclasts  are  com-
posed of thin-bedded turbiditic sediments. Some smaller ones

Fig. 2. General stratigraphic scheme of the Cretaceous—Paleocene in
the Silesian Nappe (compiled from Oszczypko 2004 and Vašíček et
al.  2010,  and  references  therein).  The  Lower  Istebna  Beds  shaded.
Position  of  the  studied  outcrops:  1  –  Łęki  quarry,  2  –  Łęki-river
and  Łęki-klippe  sections,  3  –  Czaslaw 1  quarry,  4  –  Czasław 2
quarry, 5 – Sobolów quarry, 6 – Zonia quarry, 7 – Wola Kombor-
ska quarry.

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are  built  of  sideritic  marly  mudstones.  The  upper  part  of  the
Łęki-klippe  section  contains  layers  of  conglomerates  com-
posed  of  mud  intraclasts  and  muddy  sand  matrix  (Fig. 8C).
The bases of some sandstone beds are channelized or loaded.
Individual  scours,  a  few  tens  of  centimeters  wide  and  up  to
10 cm deep, are filled with fine conglomerate or conglomerat-
ic  sandstones.  Some  beds  are  covered  by  ripplemarks  at  the
top. Locally, dish and flame structures are present. Two sand-
stone-mudstone  beds  are  involved  in  a  submarine  slump,
which is about 1 m thick. At the top, some thick beds transit
rapidly  into  a  thin  layer  of  horizontally  and/or  ripple-cross
laminated  sandy  mudstones  and  mudstones,  which  contain
abundant  carbonized  plant  detritus  (Fig. 8B,D)  and  are  com-
monly covered by jarosite varnish.

In the Czasław 1 (Figs. 1, 3A, 5; GPS coordinates:

N49°50.505

’; E020°06.857’; ±11 m) and Czasław 2 (Figs. 1,

3A; GPS coordinates: N49°50.554

’; E020°06.669’; ±5 m)

quarries,  thick-bedded,  commonly  amalgamated,  coarse-
grained, poorly sorted, arkosic sandstones with clayey, locally
siliceous  contact  pore  cement  (Bromowicz  2001)  crop  out.
They  contain  mud  intraclasts  and  armoured  mudballs,  which
are  up  to  20 cm  in  diameter.  Amalgamation  surfaces  are  un-
derlined  by  a  grain-size  change.  Dish  structures  and  sand
veins related to them are present. The veins, up to 10 cm thick,
are manifested on the bedding surface as a polygonal network
of ridges, which are up to a few centimeters high. The beds are
massive,  exceptionally  horizontally  laminated.  The  base  of
some beds is loaded. At the top, the grains are finer and a rapid
transition  to  a  thin  layer  of  horizontally-  or  ripple-laminated
sandy mudstones is common.

In the Sobolów quarry (Figs. 1, 3B, 5, 8A; GPS coordinates:

N49°53.887

’; E020°20.979’; ±5 m), thick-bedded, commonly

Fig. 3. Geological maps of the study areas. A—D correspond to the indications in Fig. 1. A – is based on Burtan (1954, 1974), B – on
Skoczylas-Ciszewska & Burtan (1954), C – on Skoczylas-Ciszewska & Burtan (1954), and D – on Mitura & Birecki (1966); all changed
and simplified.

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amalgamated,  mostly  medium-grained,  poorly  sorted  sand-
stones  crop  out.  Their  bases  are  sharp,  locally  covered  by
flute  casts.  The  cement  is  clayey,  locally  calcareous  in  the
lower  part.  The  beds  at  the  top  change  from  muddy  sand-
stone to grey or greenish grey horizontally laminated sandy
mudstones  with  plant  detritus.  In  the  lower  part  of  the  sec-
tion,  large  intraclasts  of  sideritic  mudstones  are  present
(Fig. 8F). Close to the top, small mudballs occur.

In the Zonia quarry (Figs. 1, 3B, 5; GPS coordinates:

N49°53.771

’; E020°22.023’; ±7 m), a 2.5 m thick bed of

pebble mudstone crops out in the SW limb of the Królówka
Syncline  (Skoczylas-Ciszewska  1952;  Bromowicz  2001).  It
contains quartz, lydite, sandstone, gneiss and marlstone peb-
bles in muddy and sandy matrix, sandstone intraclasts, and a
large  block  of  thin-bedded  flysch,  which  is  about  3 m  long
and 1 m thick. The bed is underlined and overlaid by thick-
bedded  conglomerates  and  coarse-grained  sandstones  that
display erosive bed bases. They contain shale intraclasts and
mudballs, which are up to 35 cm long.

In the Leksandrowa quarry (Figs.1, 3C, 5; GPS coordi-

nates: N49°53.636

’; E020°26.788’; ± 12 m), a 9.5 m thick

section  of  very  thick-  and  thick-bedded,  medium-  and
coarse-grained, poorly sorted sandstones crop out in the NE
limb  of  the  Wiśnicz  Nowy  Anticline  (Skoczylas-Ciszewska
1952). They contain shale intraclasts, which are up to a dozen
cm  thick,  and  lensoidal  laminae  of  fine-grained  conglomer-

ate. The base of some beds is channelized and filled with
coarser sediment.

In the Wola Komborska quarry (Figs. 1, 3D, 6; GPS coor-

dinates: N49°44.091

’; E021°53.566’), a 28 m-thick section

crops  out  in  the  northern  limb  of  the  Wola  Komborska
Anticline,  which  is  a  part  of  the  folded  Czarnorzeki  Anti-
cline  (Mitura  &  Birecki  1966).  Thick-bedded,  medium-
grained  sandstones  prevail  in  the  lower  part.  In  the  upper
part, also thin- and medium-bedded fine-grained sandstones
intercalated with grey siltstones-mudstones are present. Out-
crop surface dirt due to exploitation did not permit observa-
tion  of Ophiomorpha  and  possible  other  trace  fossils  in  the
lower part of the section; the trace fossils are, however, well
visible  in  cut  exploited  blocks  and  also  in  the  architectural
elements  in  Cracow  (Rajchel  2002,  2003,  2004;  Rajchel  &
Uchman 2009).

Trace fossils in thick-bedded sandstones of the

Lower Istebna Beds

The thick-bedded sandstones contain almost exclusively

Ophiomorpha rudis (Książkiewicz, 1977). Very rarely,
Zoophycos isp. and Chondrites isp. occur.

Ophiomorpha rudis (Figs. 8D, 9) was previously de-

scribed by Książkiewicz (1977) as Sabularia rudis, but was

Fig. 5. Sections of the Lower Istebna Beds in the Czasław 1, Czasław 2, Sobolów, Zonia and Leksandrowa quarries. Legend as in Fig. 4.

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sand-filled tunnels (Fig. 8D), which are partly arranged in an
irregular  polygonal  pattern  (Fig. 9C,G).  The  hexagons  are
mostly  150—200 mm  wide.  The  tunnels  are  4—14 mm  (most
often  7—11 mm)  wide.  The  branches  are  mostly  Y-shaped,
with only slight enlargement in the branching point. Vertical
or  oblique  shafts,  which  display  the  same  morphology  and
size  as  the  horizontal  galleries,  cross  thick  sandstone  beds
(Fig. 8E).  They  are  up  to  at  least  110 cm  long,  rarely
branched, and much less common than the horizontal galler-
ies.  In  some  cases,  the  shaft  crosses  more  than  one  bed.
Probably,  such  cases  and  the  length  of  the  shaft  are  under-
estimated,  because  exposure  surfaces  usually  follow  only  a
fragment  of  a  burrow  system.  Judging  from  thickness  of
some beds, which contain O. rudis in their lower part, the to-
tal  length  of  shafts  can  exceed  200 cm.  The  shafts  join  the
horizontal galleries on the lower surface of the thick beds, or
below  in  the  sandy  mudstones,  where  many  branches  run
out, sometimes in a rosette pattern. Some shafts enter larger
intraclasts and mudballs, where they can branch pointing to
reworking of their sediment. In the Czasław 1 quarry, O. rudis
crosses  dish  structures  and  up  to  8 cm-thick  sand  veins,
pointing to their early origin.

The shafts and galleries are smooth, showing sharp margins,

or are lined with ashy muddy sand, or are bounded by a more
distinct,  locally  granulated  wall  composed  of  ashy  muddy
sand  (Fig. 9A).  The  granules  are  irregularly  ovate,  1—2 mm
wide. Rarely, the lining is ferruginous (Czasław 1 and Wola
Komborska  quarries;  Fig. 9F),  probably  after  oxidized  py-
rite. The shafts and galleries are filled mostly by sandstone,
which is the same as in the thick beds, or different in grain
size, rarely enriched in plant detritus (Fig. 9B).

Zoophycos isp. (Fig. 10I) occurs only in the Łęki quarry,

5 cm below the top of a 50 cm-thick bed. It is a spreite planar
lobe, at least up to 250 mm long and at least up to 175 mm
wide. Zoophycos was produced by an unknown organism,
which collected sediment from the surface and placed it
deeply in the sediment (see Bromley & Hanken 2003; Löwe-
mark et al. 2007; and references therein for discussion). For
alternative interpretations see Olivero & Gaillard 2007).

Chondrites isp. (Fig. 10A) is present at the top of the bed

with Zoophycos isp. in the Łęki quarry and in three beds in the
Wola  Komborska  quarry.  It  is  seen  as  horizontal  to  oblique,
branched,  mud-filled,  1—2 mm  wide  tunnels.  Chondrites  isp.
is  produced  by  deeply-penetrating,  probably  chemosymbiotic
organisms (see Fu 1991; Uchman 1999, and references therein).

Trace fossils in thin- and medium-bedded flysch of

the Lower Istebna Beds

In the “Inoceramian-type flysch” (see geological setting) in

the Łęki-river section, Planolites isp., Chondrites isp., Phyco-
siphon  incertum,  Arthrophycus  strictus,  Thalassinoides  isp.,
Ophiomorpha  annulata,  O.  rudis  and  Scolicia  strozzii  have
been found. Planolites isp. is common, other trace fossils are
rare. Planolites isp. also occurs in a very thin intercalation of
greenish  mudstone  in  the  Czasław 1  quarry  and  in  greenish
grey  and  greenish  mudstones  or  on  soles  of  overlying  sand-
stone beds in the lower part of the Czasław 2 quarry section.

In the non-calcareous thin-bedded package in the higher

part of the Wola Komborska section, in loose slabs of thin-
bedded sandstones, Helminthorhaphe flexuosa was found.
Moreover, Chondrites isp. occurs here.

Arthrophycus strictus Książkiewicz, 1977 (Fig. 10D) is a

tubular, dichotomously branched, hypichnial burrow,
3—3.5 mm wide, locally covered with thin, perpendicular
striae. The branches are up to 30 mm long. For discussion of
this trace fossil see Uchman (1998).

Helminthorhaphe flexuosa Uchman, 1995 (Fig. 10B) is a

hypichnial,  1 mm  wide,  meandering  string.  The  meanders
are  at  least  40 mm  deep,  and  3.5—5 mm  wide,  and  show
gentle,  second-order  undulations.  For  discussion  of
Helminthorhaphe see Uchman (1995).

Phycosiphon incertum Fischer-Ooster, 1858 (Fig. 10E,G)

is manifested as thin, curved tunnels, 0.8—1 mm wide, which
form 3—4 mm wide and up to12 mm long lobes. For discus-
sion of Phycosiphon see Wetzel & Bromley (1994).

Planolites isp. (Fig. 10F—H) is a tubular, unlined, variably

oriented  burrow,  1.5—2 mm,  rarely  up  to  4 mm  in  diameter.
It  is  observed  as  hypichnial  semi-reliefs  (Fig. 10F)  in  sand-
stone  beds  above  shales,  or  as  endichnial  full  reliefs
(Fig. 10G—H)  in  greenish-grey  and  greenish  mudstones,
where  it  gives  spotty  fabric  (darker  oval  spots  on  lighter
background) in cross section. For discussion, see Pemberton
& Frey (1982) and Keighley & Pickerill (1995).

Thalassinoides isp. (Fig. 10F) occurs as hypichnial

branched ridges, 8—15 mm wide, which are preserved in
semi-relief. For discussion of Thalassinoides see Frey et al.
(1984).

Ophiomorpha annulata (Książkiewicz, 1977) (Fig. 10C)

is a horizontal, 2—4 mm thick, branched, sand-filled tunnel,
which was found at the base of a 12 cm thick sandstone bed.
For more data on this ichnospecies see Uchman (1995).

Scolicia strozzii (Savi & Meneghini, 1850) (Fig. 10F) is

winding,  smooth,  bilobate  hypichnial  ridge,  about
25—27 mm wide, divided by a semicircular axial furrow that
occupies most of the ridge width. The structure is preserved
in  semi-relief  in  fine-grained  sandstone  turbidites.  This
ichnospecies was described as Taphrhelminthopsis Sacco or
Taphrhelminthoida Książkiewicz in the earlier literature, but
is  considered  to  be  a  casted  washed-out  shallow  Scolicia,  a
burrow attributed to irregular echinoids (Uchman 1995).

Ophiomorpha rudis (Książkiewicz, 1977) and Chondrites

isp. display the same features as in the thick-bedded sedi-
ments (see the previous chapter).

Discussion

The presented data and the data from the literature (Ta-

ble 1) show that the trace fossil assemblage from the Lower
Istebna  Beds  is  low  in  diversity,  and  most  ichnotaxa  occur
rarely. The total of 17 ichnogenera occurring in the Campa-
nian—Maastrichtian  Lower  Istebna  Beds  is  only  half  the
number  for  the  maximum  diversity  in  flysch  sediments  at
that time (Uchman 2007).

The trace fossil assemblage in the thick-bedded sandstone is

dominated by Ophiomorpha rudis. However, it is absent in

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GEOLOGICA CARPATHICA, 2012, 63, 2, 107—120

many beds. Other trace fossils are very rare. This is probably
caused by the dominant sandy substrate, which was success-
fully colonized only by the Ophiomorpha tracemaker, proba-
bly  a  decapod  crustacean  (Uchman  2009).  Most  flysch  trace
makers lived in mud (Kern 1980; Uchman 1998). The crusta-
cean  trace  maker  of  Ophiomorpha  rudis  burrowed  deeply  to
reach  buried  muddy  sands  and  sandy  mudstones,  including
these rich in plant detritus. It is supposed that the trace maker
fed  on  the  plant  detritus  with  microbially  decomposed  cellu-
lose below the redox boundary (Uchman 2009). Probably, the
decomposed  plant  detritus  was  not  the  exclusive  diet  of  the
crustaceans.  Nevertheless,  O.  rudis  can  be  considered  as  a
domichnial-fodinichnial burrow system. The discussed assem-
blage  can  be  ascribed  to  the  Ophiomorpha  rudis  ichnosubfa-
cies  of  the  Nereites  ichnofacies,  which  is  typical  of  channel
facies  and  proximal  depositional  lobes  in  the  deep-sea  fan
models (Uchman 2001, 2009). However, more than half of the
studied  sections  do  not  show  the  characteristic  thickening/
coarsening  up  packages  typical  of  prograding  depositional
lobes  or  the  typical  thinning/fining  up  packages  typical  of
channel fills (see Mutti & Ricci Lucchi 1972; Walker 1978).
The  sections  (Figs. 4—7)  show  rather  an  aggradation  pattern
(Czasław 1 quarry, Sobolów quarry, lower-middle part of the
Łęki-klippe sections), with only occasional thin channel-type
packages  (lower  part  of  the  Łęki  quarry,  upper  part  of  the
Wola  Komborska  quarry  sections),  or  with  thin  prograding
depositional  lobes  (uppermost  part  of  the  Łęki-klippe  and
Czasław 2 quarry sections). However, the thickening-up pack-
ages can also be interpreted as the crevasse splay sediments of
meandering channels in the sense of deep-water sedimentation
(e.g.  Posamentier  &  Walker  2006).  The  aggradation-type  ar-
rangement  of  beds  fits  well  into  the  model  of  a  siliciclastic
ramp  or  apron  (Stow  et  al.  1996  and  references  therein)  that
formed in proximity to its clastic material source, as proposed
for  the  Lower  Istebna  Beds  in  the  western  part  of  the  Polish
Flysch  Carpathians  (Strzeboński  2003).  Such  deposits  are
formed  from  non-turbulent  gravitational  flows,  sandy-debris
or turbiditic flows, or cohesive debrites in the case of the peb-
ble mudstones (Strzeboński 2005). Thus, sand rich ramps and
slope  aprons,  or  crevasse  splays  can  be  added  as  new  places
for the Ophiomorpha rudis ichnosubfacies occurrence.

The medium- and thin-bedded flysch packages in the Lower

Istebna  Beds  display  the  impoverished  Nereites  ichnofacies.
Several beds do not contain any trace fossils. The presence of
the  graphoglyptid  trace  fossil  Helminthorhaphe  in  the  Wola
Komborska quarry, Helminthorhaphe and Paleodictyon in the
“Inoceramian-type facies” at Czchów (20 km SE of the area C
in Fig. 1; Table 1) suggest the Paleodictyon ichnosubfacies of
the Nereites ichnofacies, which is typical of the overchannel,
distal  depositional  lobe  and  inter-lobe  facies  (Uchman  2004;
Uchman  &  Wetzel  2011).  However,  relatively  low  diversity
(not more than three ichnotaxa in one bed) and scarcity of gra-
phoglyptids suggest the impoverished Paleodictyon ichnosub-
facies.  The  impoverishment  can  be  caused  by  lowered
oxygenation, high sedimentation rate causing frequent distur-
bances of the sea floor, and probably by limited areas of mud-
dy  sea  floor.  The  lowered  oxygenation  can  be  important  for
some  beds,  in  which  shales  display  dark  colour  and  low  de-
gree of bioturbation (Łęki-river section). Książkiewicz (1977)

mentioned that beside coarse sediments, black shales (imply-
ing low oxygenation) are the most important factors limiting
diversity of trace fossils in the Lower Istebna Beds. However,
more detailed studies on oxygenation changes in the Lower
Istebna Beds have not been done so far. Frequent disturbances
of the sea floor, for example by scouring, can limit re-estab-
lishment of ichnofauna. Most of flysch ichnofauna live in mud
(Kern 1980). Therefore, limited areas of muddy sea floor be-
tween sandy areas, provided little space for their development.

Conclusions

1. Thick- and very thick-bedded sandstones of the Lower

Istebna  Beds  contain  mainly  Ophiomorpha  rudis,  rarely
Zoophycos isp. and Chondrites isp. This assemblage is typi-
cal of the Ophiomorpha rudis ichnosubfacies of the Nereites
ichnofacies.  The  Ophiomorpha  rudis  ichnosubfacies  range
can be extended to deep-sea clastic ramps and aprons, which
are  interpreted  as  paleoenvironment  in  a  part  of  the  Lower
Istebna Beds.

2. The medium- and thin-bedded packages of flysch sand-

wiched between the thick-bedded sandstones contain  Chon-
drites  isp.,  Phycosiphon  incertum,  Planolites  isp.,
Arthrophycus  strictus,  Thalassinoides  isp.,  Ophiomorpha
annulata,  O.  rudis,  Scolicia  strozzii,  and  Helminthorhaphe
flexuosa. This assemblage, together with the published data,
is interpreted as the impoverished Paleodictyon ichnosubfa-
cies  of  the  Nereites  ichnofacies.  The  impoverishment  is  in-
fluenced  by  limited  areas  of  muddy  substrate  and  partly
influenced by lowered oxygenation.

Acknowledgments:  The  Komitet  Badań  Naukowych  (the
Polish  Committee  of  Scientific  Research)  financed  the  re-
search by A.U. in the years 2004—2006. Latter, A.U. got addi-
tional  support  from  the  Jagiellonian  University  (DS  funds).
This research was also financially supported by the Faculty of
Geology,  Geophysics  and  Environment  Protection  of  the
AGH – University of Science and Technology in Cracow –
Grant  No. 11.11.140.447.  Christian  Gaillard  (Lyon),  Radek
Mikuláš  (Prague)  and  Jozef  Michalík  (Bratislava)  provided
helpful reviews.

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