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Field guidebook
Geology of the Zittau Mountains
6
th
-7
th
of June 2017

1
Saxon part
Dr. Thomas Voigt
-------------------------------------------------------------------------------------------------------------------------
Titel figure:
Flat lying conglomeratic sandstones with intercalated conglomerate beds at
the Nonnenfelsen (Middle-Turonian, Oybin Formation), Zittau Mountains

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1. Introduction
The marine intracontinental Bohemian Cretaceous Basin in Central Europe (Fig. 1) has a
northern prolongation in Germany (Saxony) which is characterized by high thickness and
close position to a major fault, which was active during deposition of the Cretaceous
sequence and let in consequence to thrusting of the ancient source area on the adjacent
basin (Lausitz Thrust). Activity of this fault started in late Cenomanian (indicated by a source
area in the northeast and enhanced thickness in a NW-SE-striking fore-deep (marginal
trough) as was recognized by TRÖGER (1964). Like elsewhere in Central Europe, this NW-
SE-directed fault is related to uplift of the source area and deposition of a thick sequence of
Cenomanian to Santonian deposits, summarized as late Cretaceous basin inversion (e. g.
KOCKEL 2003).
Fig. 1:
Overview map of Lausitz-Krkonosze High and the surrounding basins during Turonian. Distribution of
sandstones reflects clearly uplift of an isolated source area which was later thrusted onto the basin
margins. All known deposits are of marine origin; thickness is highest close to the source area, pointing
to the formation of marginal troughs. Both the Elbsandsteingebirge and the Zittau Mountains represent
depositional systems close to the basin margin. (Figure redrawn from Voigt 2009).
The Saxonian part of the Bohemian Cretaceous basin is restricted to a 20 to 5 km wide
remnant of the primary sediment occurrence. The Lausitz Thrust cuts oblique to the marine
facies belts (fig. 1). Younger uplift of the Erzgebirge caused NE-directed tilting of the

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basement and widespread denudation at the eastern basin. Hemipelagic marls and
limestones in the NW are well-dated (biostratigraphy based on inoceramids and ammonites)
and comprise a succession from Lower Cenomanian to the Lower Coniacian (TRÖGER 2003).
Marginal coastal sandstones comprise probably the same stratigraphic interval; but to the
SE, these deposits are nearly completely represented by quartz sandstones of low fossil
content. They form a spectacular landscape of canyons and vertical rock walls
(Elbsandsteingebirge, “Sächsische Schweiz”). A second part of the marginal Bohemian
Cretaceous Basin in Saxony is represented in the area of the Zittauer Gebirge (Zittau
Mountains). Very proximal conglomeratic deposits in the Cenomanian and Turonian are
followed by finer-grained sediments of Upper Turonian and Lower Coniacian age which are
very different from the sections in the Elbsandsteingebirge and were therefore considered
always separately (e. g. ANDERT 1929, TRÖGER 2008).
The stratigraphic position and correlation of these units between the regions of coastal
deposits in Saxony (Sächsische Schweiz and Zittauer Gebirge) and the marginal parts of the
Bohemian Cretaceous Basin are still in debate, because biostratigraphic data are sparse and
lithostratigraphic correlations come to an end in the uniform and monotonous successions of
coarse sandstones and conglomerates.
Investigations in the course of the EU-funded project GRACE (Groundwater Absence in
Cretaceous Aquifers) gave already the opportunity to re-examine wells and surface outcrops.
To interpret groundwater flow in the subsurface of the Bohemian Cretaceous basin, a correct
geological model is essential. Therefore, stratigraphic correlation within the basin has to be
revised and the extension of aquifers and aquitards together with their possible connections
were investigated on the base of field observations and borehole data.
2. Lithostratigraphy of the Zittau mountains
In contrast to the southern Elbsandsteingebirge, which is characterized by a gently NE-
dipping succession, the structural pattern of the Zittau mountains in eastern Saxony is much
more complicated by Neogene volcanics (dykes, sills, intrusions, diatreme structures), and
faults related to the north-eastern end of the Ohre-Graben (fig. 2). The succession is very
monotonous in the lower part and poorly exposed in the upper units. No complete section
exists, because preservation of youngest deposits (Coniacian) is related to the graben
structure. Cenomanian deposits are not exposed at the surface on the German side. Early
Turonian deposits are only accessible at the bottom of two deeply incised river valleys close
to the Lausitz Thrust.

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Fig. 2:
Geological Map of the Cretaceous in the Zittau Mountains. In the eastern part, deposits from Upper
Turonian to Lower Coniacian are exposed (Brezno Formation). The western part consits mainly of Middle
Turonian deposits of the Oybin Formation and Lückendorf Formation (Jizera Formation, Teplice
Formation).
Cretaceous sediments of the Zittau Mountains represent the most proximal area of the
Bohemian Cretaceous basin which is expressed in a dominance of coarse-grained massive
sandstones and intercalated conglomerate sheets of 0.5 to 2 m thickness over a major part
of the section. Only one borehole was completely cored and well documented (Lückendorf
1/63; TRÖGER 1964), while some uranium-exploration wells were focused exclusively on the
basal units (fig. 3). The succession starts with Cenomanian coarse-grained sandstones of
the Oberhäslich Formation. The fluvial to estuarine deposits of the Niederschöna Formation
are probably absent in the whole area. Boreholes provided a very homogeneous facies with
two intercalated horizons of fine- to medium-grained sandstones representing probably
equivalents the Upper Cenomanian Dölzschen (upper Peruc Korycany) Formation and the
base of the Lower Turonian Briesnitz (Bila Hora) Formation. They have no clear border to the
underlying and overlying sequence, so that the basal unit is considered as the Upper
Cenomanian Oberhäslich Formation (VOIGT & TRÖGER 2000). The overlying succession
forms steep rock walls at the surface and contains only rarely fossils. TRÖGER & VOIGT
(2000) summarized these conglomeratic sandstones as Oybin Formation, corresponding to
the Jizera Formation. According to the sparse fossil record, they comprise Early and Middle
Turonian age (ANDERT 1929). Thickness exceeds 400 m (fig. 3). Depositional environment is
clearly related to a high-energetic marine environment, because cobbles show sometimes
borings of marine organisms and contain molds of shell debris. VOIGT (2012) interpreted the

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coarse (conglomeratic) layers as proximal storm beds and the poorly sorted sandstones as
amalgamated tempestites of weaker storm events, homogenized by burrowing marine fauna.
The Oybin Formation unit is overlain by calcareous fine-grained sandstones with intercalated
coarser, mostly poorly sorted sandstones. Bioturbation by decapod crustaceans is common.
This unit is about 30 m thick and becomes finer to the top, resulting in sandy marlstones
(fig. 6). According to the fossils this unit is of late Turonian age (ANDERT 1932, TRÖGER
2008). These carbonate-cemented sandstones and marlstones are summarized as
Lückendorf Formation, corresponding either to the uppermost Jizera Formation or to the
Teplice Formation. Although the upper marly parts of the formation were not exposed in the
last 90 years, interpretation as a deeper shoreface environment is the most convincing
version. The borehole Lückendorf 1/1963 is the type section, but only the lower part of this
unit was cored.
The transition to the Lower Coniacian Waltersdorf Formation was previously unknown, but in
the course of our investigations during GRACE project, the short documentation of the
borehole Waltersdorf 1930 allowed the recognition of the Lückendorf Formation at the base
of the Waltersdorf Formation (fig 6). In this borehole 23 m of marlstones above sandstones
were described which follow above typical sandstones of the Lückendorf Formation. The
uppermost part contains 8 m of a marlstone sandstone succession and 10 m of fine-grained
sandstone. These sandstones are exposed in the same altitude in the adjacent Sonnenberg
quarries and are considered as the Waltersdorf Formation.
The latter is composed of fine- to medium-grained sandstones, mostly bioturbated or
sometimes cross-bedded, separated by sharp-bounded coarse units. These well-sorted
gravelly, sheet-like beds have erosive bases, show sometimes oscillation ripples and are
followed by clay to silty layers. Like the very similar facies of the Postelwitz Formation, the
depositional system is interpreted to represent a deeper shore face environment with
proximal storm beds (VOIGT 2012). Abundant fossils allow a good biostratigraphic control.

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Fig. 3:
Log of the Borehole Lückendorf 1/1960 after the detailed documentation of Tröger and Wolf (TRÖGER
1964).The complete borehole consists of sandstone of varying grainsize. Even the marly units of the
Briesnitz Formation (Labiatus-Pläner; basal Bila Hora Formation) are replaced by sandstones.

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Large abundant quarries and some rock walls at the slope of the Lausche Mountain allow the
subdivision in three parts: the bioturbated, fossil-rich sandstones are defined as Sonnenberg
member. A rich marine fauna dominated by bivalves and echinoids yields the inoceramids
Mytiloides scupini
,
Mytiloides carpathicus
and
Inoceramus lusatiae
in the lower part indicate
a latest Turonian age (HEINZ 1929, TRÖGER 2008).
Fig. 4:
Section of the Borehole Waltersdorf 1930, redrawn after the short description (core?). The borehole is
situated close to the Lausitz Thrust at the foot of the Lausche and probably represents the transition from
the Oybin Formation to the Lückendorf Formation

8
Cremnoceramus rotundatus
and
Cremnoceramus waltersdorfensis
in the upper sections of
the quarries are typical of Early Coniacian (WALASZCZYK 1996). They are followed by
massive medium- to coarse-grained sandstones (Lausche member) without fossils. These
sandstones are moderately sorted and cross-bedded. Thickness is about 50 m. They are
well exposed at the northern slope of the Lausche (Luž). Terraces with wet lands between
the 5-10 m thick massive sandstone beds might point to thinner intercalations of finer
sandstones or marlstones. The Hochwald member is probably on top of these deposits, but
the lack of outcrops makes correlation difficult. In particular, the northern slope of the
Hochwald Mountain (Hvozd) lacks any exposure and a fault probably runs between the
Upper Turonian of Lückendorf and the much younger deposits on the southern slope of the
Hochwald. Sandstones, exposed in a few quarries on the Czech southern side of the
mountain are again characterized by bioturbated sandstones with coarse intercalations.
According to findings of
Cremnoceramus crassus
it represents the highest Lower Coniacian
and is therefore younger than the sections at the Lausche. Nevertheless, the contact of the
Hochwald sandstone to the older units is unknown, because the slopes of the Hochwald
Mountain are covered by volcanic debris of a major phonolithe body on top of the mountain.
MÜLLER (1932) mapped additionally a several meters thick claystone unit on top of the
Hochwald Mountain (Hvozd), but the section is now completely covered by phonolithe debris.
According to TRÖGER (2008), findings of
Cremnoceramus erectus
in these marlstones are
typical of late Early Coniacian.
It has to be emphasized that a new mapping of the whole area would be essential for both
better understanding of stratigraphy and tectonics in this area.

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Fig. 5:
Lithology of the Cretaceous in the Zittau Mountains, based on the combination of some well-documented
boreholes and several sections allows the correlation with the standard section of the better known
Czech side (sheet Dolni Podluži).

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Fig. 6:
Combined simplified section of the Cretaceous in the Zittau Mountains. The compilation of several
sections allows the correlation with the standard section of the better known Czech side of the Lausche
(Dolní Podluži).

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3. Tectonics and volcanics
The major fault, controlling distribution of rocks in this region, is the Lausitz Thrust which runs
roughly in E-W direction (fig. 2). It marks the boundary of the basement to the Cretaceous
basin and should incline normally with an angle between 25-30°. Nevertheless, much of the
inverted normal faults in the Central European basin preserved their initial inclination of the
extensional phase and are much steeper (e. g. KLEY 2013).
Tilting of Cretaceous units close to this thrust points either to the formation of a frontal
syncline or to additional faults striking parallel to the Lausitz Thrust. As no flattening of dip
angles were mapped until now, the cross-sections in fig. 7 show faults. To solve this
question, detailed mapping is necessary.
A second, younger fault system is represented by the Ohre rift, and accompanying basaltic
dyke systems. The main fault separates a young western unit (Lausche, Luž and
Sonnenberg) with Cretaceous sediments of Upper Turonian to Lower Coniacian age from a
western unit (Johnsdorf, Oybin, Lückendorf), composed of Lower to Upper Turonian units in
the surface outcrop. The amount of down-throw of the eastern unit is estimated to be in the
order of 400 m; the fault is interpreted to be a normal fault with a dip angle of about 60°.
The high thicknesses of monotonous, conglomeratic sandstone units make the recognition of
minor faults difficult. Nevertheless, rapid changes in dip angles and lack of correlation on
opposite sides of the valleys indicate faulting in NE-SW direction, parallel to the orientation of
basaltic dykes. These dykes of several metres thickness cut through the succession but they
are rarely exposed. Instead, hydrothermal water and subsequent weathering caused the
transformation into clay minerals. The Felsengasse between Lückendorf and Oybin and the
millstone quarries near Jonsdorf are the most prominent features of those basaltic dykes.
The only evidence of their existence is the impregnation of the sandstones with mobilized
quartz and iron oxides, columnar jointing of sandstones and some relictic, completely altered
basalts.
Phonolites occur as intrusions, the Lausche represents a complex volcanic structure, which
was investigated very recently by WENGER ET AL. (2017).
In the course of the GRACE project, several cross-sections were constructed on the base of
old maps, punctual field observations and boreholes. They reflect the recent state of
knowledge, but will probably revised after new field work.

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Fig. 7:
NS-directed cross-sections across the Lausitz Thrust and the Zittau Mountains show the thick
stratigraphic succession of the Cretaceous. Thickness at the Hochwald and the Lausche Hill might
exceed 1000 m.

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Fig. 8:
Position of boreholes and cross-sections used for Fig. 7.
Fig. 9:
Digital elevation model of the Lausche Hill area (shaded relief, data from Staatsbetrieb
Geobasisinformation und Vermessung Sachsen). Morphological features marked by coloured arrows
indicate limits of geological units. Green: horizontal cuestas of Upper Cretaceous sandstone (Waltersdorf
Formation, Lausche sandstone); Orange: sudden limits of sandstone cuestas mark the crater edge of a
maardiatreme volcano; Yellow: deep erosional grooves cut through unconsolidated material filling the
maar-diatreme; Blue: sharp margin of the lava flow; Beige: notable change in slope angle along the base
of the phonolite dome due to differing internal structure and erodibility of rocks. Coordinates according to
DHDN/3-degree Gauß-Krüger zone 5. Figure from WENGER ET AL. (2017).

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Fig. 10: Geological map of the Oligocene Lausche Volcano. Geological ages of the rocks: 8 is Lower Coniacian;
7 and 12 are Middle Paleocene–Lower Eocene (62–50 Ma); 6 is Lower Oligocene (slightly older than
30.75 ± 0.56 Ma); 3–5 are 30.75 ± 0.56 Ma; 1, 2, 9 and 11 are 29.05 ± 0.12 Ma; 10 is Lower Oligocene
(slightly younger than 29.05 ± 0.12 Ma). See Fig. for cross-section A – A′ Coordinates according to
DHDN/3-degree Gauß-Krüger zone 5. Figure from WENGER ET AL. (2017).

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Fig. 11: Reconstructed geological cross-section of the Oligocene Lausche Volcano. A relic of the pre-volcanic
surface is marked by granite debris which is preserved by the covering phonolite dome. Weak colouring
illustrates erosion since the time of volcanism. See Fig. 10 for position of cross-section A – A′. Figure
from WENGER ET AL. (2017).

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Excursion stops in Saxony
1. Teufelsmühle: Lausitz Thrust, Cambrian granodiorite, Lower Turonian sandstones
(Oybin Formation)
2. Gratzer Höhle: Oybin Formation, Middle Turonian, coarse conglomerates,
conglomeratic sandstones
3. Castle Oybin: Oybin Formation, conglomeratic sandstones
4. Felsengasse, Kelchstein: Jizera Formation, influence of hydrothermal water on
sandstones
5. Foresters House Lückendorf: Lückendorf Formation: calcareous sandstones with late
Turonian fossils, correlating to the Teplice Formation
6. Jonsdorf, Mühlsteinbrüche: weathered dykes, columnar jointing of sandstones (Jizera
Formation)
7. Waltersdorf, Sonnenberg: Waltersdorf Formation, fossilrich fine to medium grained
sandstones with inoceramids of late Turonian age
8. Lausche, Steinbruchweg:
diatreme, phonolite intrusion, Waltersdorf Formation:
sandstones of the Sonnenberg member, Lausche sandstone

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Fig. 12:
Excursion stops in Saxony

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18
Saxony - Stop 1
Location:
Teufelsmühle - Lausitz Thrust
Stratigraphy:
Cambrian granodiorite, Lower Turonian sandstones (Oybin Formation)
Things to observe:
fresh granodiorite in close relation to strongly jointed and silicified
sandstones of the Oybin (Jizera) Formation, age probably Lower
Turonian
Fig. 13: Map of the excursion area and the changing direction of the Lausitz Thrust. In contrast to other regions of
the basin, the Cretaceous sandstones are higher than the thrusted Lausitz granodiorite.

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Saxony - Stop 2
Location:
Gratzer Höhle (sandstone rock near Teufelsmühle)
Stratigraphy:
Oybin Formation, Middle Turonian
Things to observe:
coarse conglomerates, conglomeratic sandstones, conglomerates
consists of sandstones, ironstones and limonitic sandstones; no
granodiorite!, tectonic thrust-related features
Interpretation:
The absence of granodiorite pebbles is of striking evidence for
inversion of a sedimentary basin which was on top of the later Lausitz-
Krkonosze High.
Fig. 14: Several generations of displaced joints
Fig. 15: Conglomerate bed of quartz pebbles
Fig. 16: Reworked sandstones and ironstones

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Saxony - Stop 3
Location:
Castle Oybin
Stratigraphy:
Oybin Formation, Middle Turonian
Things to observe:
conglomeratic sandstones, conglomerate beds mainly composed of
quartz; marine sandstones of an high energetic environment, probably
wave agitated, conglomeratic sandstones are the result of bioturbation
Fig. 17: Flat lying deposits of the Oybin Formation, corresponding to the Jizera Formation. Layering is marked by
conglomerate beds which have lower weathering resistivity than the conglomeratic sandstones.

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Saxony - Stop 4
Location:
Felsengasse, Kelchstein between Oybin and Lückendorf
Stratigraphy:
Jizera Formation
Things to observe:
sandstones with only few pebbles, red coloured, jointed, impregnation
of iron oxides, trace of a weathered basaltic dyke
Interpretation:
Intrusion of a thick basaltic dyke caused late diagenetic alteration, also
the red colour is a secondary feature
Fig. 18: Kelchstein, the most impressive rock in the Felsengasse, consists of red colored sandstones of the
Oybin Formation. Some surfaces show impregnations of iron oxides.

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Saxony - Stop 5
Location:
Foresters House Lückendorf
Stratigraphy:
Lückendorf Formation (Teplice Formation)
Things to observe:
calcareous sandstones with late Turonian fossils, correlating to the
Teplice Formation?
Interpretation:
deeper shore face, normal marine, storm influence, bioturbation
dominant
Fig. 19: EW-cross-section of the Oybin area towards Lückendorf shows the vertical displacement of the eastern
units (about 80 m according the borehole data).

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Saxony - Stop 6
Location:
Jonsdorf, Mühlsteinbrüche
Stratigraphy
:
Jizera Formation
Things to observe
: massive, partly silicified sandstones weathered dykes, columnar
jointing of sandstones, canyon was formed by weathering of a thick
basaltic dyke
Fig. 20: gorge near Jonsdorf
Fig. 21: Columnar jointing of sandstones proves the former existence of a basalt dyke.

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Saxony - Stop 7
Location:
Waltersdorf, Sonnenberg
Stratigraphy:
Waltersdorf Formation (Brezno Formation)
Things to observe:
fossil-rich, fine- to medium grained sandstones with inoceramids of late
Turonian age, claystone layers
Interpretation:
storm-dominated environment of the deeper shoreface
Fig. 22: Abandoned sandstone quarry at the slope of the Sonnenberg (Waltersdorf Formation)
Fig. 23: Late Turonian inoceramid from the Sonnenberg sandstone

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Saxony - Stop 8
Location:
Lausche, Steinbruchweg
Stratigraphy:
Waltersdorf Formation (Brezno Formation): Sonnenberg member,
Lausche sandstone
Things to observe:
fossilrich, fine- to medium grained sandstones with inoceramids of late
Turonian age, claystone layers, overlain by 8 horizons of thickly
bedded, coarse-grained sandstones; diatreme, phonolite intrusion
Interpretation:
storm-dominated environment of the deeper shoreface, progardation
and transition to upper shoreface sandstones
Fig. 24: Abandoned sandstone quarry at the slope of the Lausche (Sonnenberg sandstone)
Fig. 25: Massive sandstones (Lausche sandstone) of the higher Waltersdorf Formation.

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References
ANDERT, H. (1929): Die Kreideablagerungen zwischen Elbe und Jeschken II. Die
nordböhmische Kreide zwischen Elbsandsteingebirge und Jeschken und das Zittauer
Sandsteingebirge. – Abh. Preuß. Geol. Landesanst., 117: 1-227, Berlin.
HEINZ, R. (1929): Zur stratigraphischen Stellung der Sonnenbergschichten bei Waltersdorf in
Sachsen (westsüdwestlich von Zittau). Beiträge zur Kenntnis der oberkretazischen
Inoceramen IX. – 23. Jber. Nieders. geol. Ver.: 22-53, Hannover.
KOCKEL, F. (2003): Inversion structures in Central Europe - expressions and reasons, an
open discussion. – Netherlands J. Geosciences: Geologie en Mijnbouw, 82(4): 367–
382, Utrecht.
LAMPRECHT, F. (1927): Schichtenfolge und Oberflächenformen im Winterberggebiete des
Elbsandsteingebirges. – Mitt. Ver. Erdkunde Dresden, N.F., Jg. 1927: 1–48.
MALKOVSKY, P. (1987): The Mesozoic and Tertiary basins of the Bohemian Massif and their
evolution. – Tectonophysics, 137: 31-42.
MÜLLER, R. (1932): Die geologische Sektion Deutsch-Gabel des Kartenblattes Rumburg-
Warnsdorf. – Sbor. Geol. úst. CSR, sv. VIII, roc. 1928-1929, Praha.
PRESCHER, H. (1981): Probleme der Korrelation des Cenomans und Turons in der
Sächsischen und Böhmischen Kreide. – Z. geol. Wiss. 9: 367-373.
TRÖGER, K.-A. (1964): Die Ausbildung der Kreide (Cenoman bis Coniac) in der Umrandung
des Lausitzer Massivs. – Geologie, 6/7: 717–730, Berlin.
TRÖGER, K.-A. (2008): Kreide – Oberkreide. – In: PÄLCHEN, W. & WALTER, H. (2008) eds.:
Geologie von Sachsen. 311-358. Stuttgart.
TRÖGER, K.-A. & VOIGT, T. (2000): Sachsen. – In: Stratigraphische Kommission Deutschlands
(Hrsg.): Stratigraphie von Deutschland III. Die Kreide der Bundesrepublik
Deutschland. 123-132, Frankfurt.
VOIGT,
T.
(2009):
Die
Lausitz-Riesengebirgs-Antiklinalzone
als
kreidezeitliche
Inversionsstruktur: Geologische Hinweise aus den umgebenden Kreidebecken. – Z.
Geol. Wiss., 37: 15–39.
VOIGT, T. (2011): Sturmdominierte Sedimentation in der Postelwitz-Formation (Turon) der
Sächsischen Kreide. – Freiberger Forsch.-H., C 540 (Karl-Armin-Tröger-Festschrift):
3–25.
ULIČNÝ, D. (2001): Depositional systems and sequence stratigraphy of coarse-grained deltas
in a shallow-marine, strike-slip setting: the Bohemian Cretaceous Basin. –
Sedimentology, 48: 599–628.
VALEČKA, J. (1984): Storm surge versus turbidite origin of the Coniacian to Santonian
sediments in the eastern part of the Bohemian Cretaceous Basin. – Geologische
Rundschau, 73(2): 651-682.
WALAZSZYK, I. (1996): Inoceramids from Kreibitz-Zittauer area (Saxony and northern
Bohemia): revision of ANDERT´s (1911) descriptions. – Paläont. Z., 70 (3/4): 367-
392, Stuttgart.

27
Czech part
Česká geologická služba

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4. Lužice Fault
The most prominent tectonic structure along the NE border of the Bohemian Cretaceous
Basin is Lužice (Lausitz) fault (LF). The tectonosedimentary evolution of the basin can be
divided into three stages: early to middle Cenomanian, latest Cenomanian to late Turonian
and Coniacian to early Santonian (ULIČNÝ ET AL. 2003). During second stage the Lužice
(Lausitz) -Jizera sub-basin was evolved. The activity along this tectonic line started in Late
Cretaceous and continues to Cenozoic. The dominant movement and deformation are
documented in the Late Cretaceous to Paleocene (ADAMOVIČ & COUBAL 1999). The oldest
deformational structures have character of folds and flexures. The vertical movements in the
middle part of the LF (Saxony in the Zittau-Oybin area and Czech part near Hrádek n. N and
Jítrava) coincide with the period of the volcanic activity of the Ohře (Eger) Graben. The uplift
of the Cretaceous sediments in this area is the result of the tectonic activity of Pliocene or
younger age along of the FL and NE-SW and E-W-striking faults (KRENTZ & STANEK 2015).
Fig. 26: Position of the excursion localities in the Czech part of the study area

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The Czech stop 1 and 2 document these vertical tectonic movements along LF (Fig.27).
Fig. 27: Position of the excursion localities in the geological map 1 : 50 000

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30
Czech Republic – Stop 1
Location:
Kohoutí vrch (former Lipový vrch)
Stratigraphy:
Middle to Upper Turonian Jizera Formation
The Kohoutí vrch hill, formerly Lipový vrch hill, runs northeastward from the triangulation
point Sedlecký Špičák (544 m a. s. l.), situated SSE of Hrádek nad Nisou near the border
with the Free State of Saxony. The whole hill consists of Cretaceous quartz sandstones
(Quadersandsteine) and conglomerates of the Jizera Formation of mid to late Turonian age.
In the vicinity of the Lusatian Fault they have been silicified. The almost vertical layers of
those sediments are well-exposed at impressive sandstone walls on the hill ridge and exhibit
slickensides (fault polish) that are due to tectonic movements along the Lusatian Fault. This
outstanding tectonic line runs parallel to the ridge and separates the Cretaceous sediments
from the northeastern up-thrown block represented by granodiorite of the Lusatian Pluton
(the medium-grained Zawidów type). Crystalline rocks occur on the northeast slope only in
the plough scatter, regular outcrops are found only along the newly upgraded forest road
above the Bílý potok (Weissbachtal) valley.
The resistant sandstones were extracted as building stone in several large quarries, merging
together and surrounding the top of the Kohoutí vrch hill from three sides. The extraction
stopped probably in the 1st half of the 20th century, today, the quarries have been
abandoned and overgrown by woods. Near an old path on the northern slope of the Kohoutí
vrch hill, there stood a pub, Volkertbaude, called after its owner. It was a stone-built mountain
cottage with a large sun roof providing a majestic scenic view of the land along the Neisse
River.
Fig. 28 and 29: Locality Kohoutí vrch
Cretaceous sandstone (left) on the top of hill and outcrop of the
granodiorite on the northeast slope (right).

image
image
31
Czech Republic – Stop 2
Location:
Ostrý vrch hill (Kozí hřbety/Ziegenrücken)
Stratigraphy:
Middle to Upper Turonian Jizera Formation
Southeast of Horní Sedlo, an about 2 km long range is situated, having on its top an
important geological boundary, called Lusatian Fault. The times after Cretaceous
sedimentation were marked by an uplift of the northeastern block in relation to the
southwestern, downthrown one. The opposite motion of the two blocks on the Lusatian Fault
caused the originally horizontal beds of the Jizera Formation (Middle to Upper Turonian) near
the Fault having been bent into an obliquely dipping almost vertical position. This led
subsequently to intense erosion on the up-thrown northeastern block so that at present,
phyllites, green-schists and meta-dolerites of the Ještěd Crystalline complex (Krkonoše-
Jizera Unit) occur on the surface.
They are of late Devonian to early Carboniferous age and represent the Cretaceous
basement. A nameless hilly area occurs southeast of the Ostrý vrch hill built by sandstone
walls with steeply dipping beds. One of the walls displays the so called slickenside with fault
polish.
Fig. 30 and 31:
Locality Ostrý vrch hill: Cretaceous sandstone
in the vertical position along the Lusatian fault (left) on the
contact with outcrop of the phyllites and green schists (right) of
the Ještěd Crystalline complex.
Underneath the hill top there is a group of old quarries, where sandstone was extracted for
construction purposes. The stonemasons cut not only rectangular blocks out of it, or door
lining and stairs but also sculptures, ornamental portals, stone vases and other decorations.
The quarrying boomed at the turn of the 18th and 19th centuries, as the stone material was

32
hauled to Liberec to build large houses for its wealthy citizens. The quarrying continued until
1835, but gradually it ceased to be a paying business and the quarries were abandoned.
Besides sandstones, also coarse-grained conglomerates with bigger pebbles occur,
displaying numerous molds of Mesozoic pelecypod shells in many places.

image
33
Czech Republic – Stop 3
Location:
Bílé kameny (White stones)
Stratigraphy:
Middle to Upper Turonian Jizera Formation
The Bílé kameny site forms an isolated, morphologically outstanding rock group ca. 1 km
north of Jítrava, at the foot of the Vysoká hill. They strike one´s eyes by their white color and
rounded forms, reminding of formidable backs of resting elephants, sometimes being called
Sloní skály (Elephant´s rocks). Since they are an exhibit of unusual weathering pattern of
Cretaceous sandstones they were given protected status in 1955.
They are made up of quartz sandstones (Quadersandsteine). The uniform petrographic
composition and grain size have given rise to their displaying rounded, mushroom-shape or
regular ball-shape forms, in particular in the apical parts of the rock outcrops. They are
medium-grained to coarse-grained and diagonal bedding developed at some horizons. They
belong to the Jizera Formation and are of mid Turonian to late Turonian age.
Fig. 32: Locality Bílé kameny (White stones or Elephant´s rocks).
AFTER MACKOVČIN ET AL. (2002): “originally horizontal beds were uplifted and tilted on the
Lusatian Fault”. Upper part of the sandstone sequence is marked by high proportion of the
kaolinite cement in the intergranular space and poorly developed bedding. These lithologic
properties gave rise to the unusual weathering pattern described above. At the top of one of
the rocks a well-developed oval-shaped rock pan occurs with a draining flute. Another point
of interest is several small pseudo-karst caves and cavities generated by selective
weathering and erosion of coarser-grained layers in the sandstones. At present, the Bilé
kameny rock group is divided by three broad, almost vertical fractures into a number of

34
independent rock blocks, forming a small rock city. Oval-shaped cavities and caves, the
longest being ca. 6 m long, developed on the rock walls or at their footwall due to the
selective weathering of less resistant sandstone layers. One of the rock walls contains a
small, more than 4 m long rock tunnel.

35
References
ADAMOVIČ, J.– COUBAL, M., (1999): Intrusive geometries and Cenozoic stress history of the
northern part of the Bohemian Massif.
GeoLines 9
, 5–14.
KRENTZ, O. – STANEK, K. (2015): Die Lausitzer Űberschiebung zwischen Meissen und
Jeschen – neue Aspekte. – Berichte der Naturforschenden Gesellschaft der
Oberlausitz, Band 23, pp. 123-137, Gőrlitz.
ULIČNÝ, D. – ČECH, S. – GRYGAR, R. (2003): Tectonics and depositional systems of a shallow-
marine, intra-continental strike-slip basin: exposures of the Český Ráj region,
Bohemian Cretaceous Basin.
GoeLines 16
, 133–148.