Palaeogeography and tectonic structure of allochthonous units in the German part of the Rhenohercynian Belt: revision and comment
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Int J Earth Sci (Geol Rundsch) (2006) 95: 168–172
DOI 10.1007/s00531-005-0512-1
COMMENT
H. Hüneke
Palaeogeography and tectonic structure of allochthonous units
in the German part of the Rhenohercynian Belt: revision and comment
Received: 10 November 2004 / Accepted: 14 April 2005 / Published online: 16 June 2005
Springer-Verlag 2005
Huckriede et al. (2004) proposed new information on tectono-sedimentary units. According to the Gauss-
palaeogeography, orogenic evolution, tectonic structure, Krüger coordinates given by the authors (Table 1 of
and boundaries of allochthonous units in the Rhenoh- Huckriede et al. 2004), only two samples are from the
ercynian Belt, which is mainly based on provenance Harzgerode Zone and at least seven samples are from
analysis of clastic sediments. The interpretation, inte- the Blankenburg Zone. A revised database is shown in
grating 40K/40Ar cooling ages of detrital muscovites and Table 1.
stratigraphic data, is validated by comparing the results The second problem is the selection of sample
with known muscovite ages from possible source regions. localities. Unfortunately, the 40K/40Ar determinations
With respect to the Blankenburg and Harzgerode of muscovites from pre-flysch deposits were performed
Zones, which are part of the allochthonous Harz Nappe only in some cases on stratigraphically well-dated suc-
(Walliser and Alberti 1983), the interpretation given is cessions. Based on a single tentative and unpublished
doubtful. The siliciclastic sedimentary record of the palynological analysis of one sample from the northern
Blankenburg Zone is interpreted to be derived from edge of the Harz (Hg 225), five further samples
Laurussia (Old Red Sandstone Continent) in analogy from various localities and sedimentary formation of
with the par-autochthonous shelf sediments of the Rhe- different tectono-sedimentary units are attributed to
nohercynian Belt, whereas the siliciclastic sedimentary the Ordovician (Hg 227, Hg 210, Hg 166 and Hg
record of the Harzgerode Zone is interpreted to be derived 235). Without further biostratigraphic investigations,
from Armorica, and, moreover, the tectono-sedimentary this assumption is highly speculative and ignores
unit itself is assigned to Armorica. Both the Blankenburg published and unpublished biostratigraphic data (see
and Harzgerode Zones are considered to represent totally Table 1).
different tectono-sedimentary units and terranes, which The 40K/40Ar determinations of detrital muscovites
contradicts the hitherto published data. Stratigraphic and from pre-flysch deposits of the Harz Mountains reveal
sedimentologic investigations have generally revealed the ages between 412 Ma and 610 Ma, which may be
nearly identical sedimentary record preserved within attributed to two age clusters (Table 2): (i) Silurian to
these units (e.g., Schriel 1954; Möbus 1966; Lütke 1978; Early Devonian muscovite ages (440–410 Ma) and
Walliser and Alberti 1983; Wachendorf 1986; Alberti (ii) Late Proterozoic muscovite ages (760–540 Ma).
1995; Wachendorf et al. 1995; Hüneke and Weller 2003). There is no doubt that Silurian to Early Devonian
The purpose of this comment is to highlight critical muscovite ages characterize sediments from Caledonian
aspects and arguments in the validation and confusion uplifts of Laurussia. The siliciclastic detritus was trans-
in the original data sets for the Harz Mountains pro- ported across the Avalonian foreland and was deposited
posed by Huckriede et al. (2004). on the shelf adjacent to the south. However, it is more
First, six of the 11 pre-flysch samples investigated difficult to interpret the significance of the Late Prote-
from the Harz Mountains are wrongly attributed to the rozoic muscovite ages and to reveal the provenance of
the mica-bearing siliciclastic detritus preserved within
the Blankenburg and Harzgerode Zones. They imply
H. Hüneke four different interpretations:
Institut für Geographie und Geologie,
Universität Greifswald, Jahn-Strasse 17a, 1. Late Proterozoic muscovite ages of Devonian sand-
17487 Greifswald, Germany
E-mail: hueneke@uni-greifswald.de
stones probably characterize Cadomian detritus from
Tel.: +49-3834-864567 metamorphic units produced and exhumed during
Fax: +49-3834-864572 the Cadomian orogeny at the northern margin of169
40 40
Table 1 K/ Ar analyses of detrital muscovites from the Harz Mountains (Huckriede et al. 2004) showing revised assignments to
tectono-sedimentary units and additional biostratigraphic data
40
Sample Locality (Gauss-Krüger Stratigraphy and petrography K/40 Ar age, Tectono-sedimentary units,
coordinates) 2r-error (Ma) lithostratigraphy, and
biostratigraphy
Hg 167 Badeholz near Harzgerode Late Devonian or Early 396±08 Harzgerode Zone: Cyclostigmen-Schichten
(Harzgerode Zone) R4438000 Carboniferous: greywacke (Ruchholz et al. 1973)
H5722800
Hg 212 Treseburg (Blankenburg Zone) Middle or Late Devonian: 414±17 Blankenburg Zone: ?Bodetal-Olisthostrom
R4428700 H5732600 quartz–sandstone (Lutzens and Schwab 1972) or Quarzit
von Wienrode-Altenbrak ? (Weller 1968;
Borsdorf 1975); Eifelian or Givetian (see
Schwarz 1982; Fehlauer 1991)
Hg 213 Altenbrak (Blankenburg Zone) Middle or Late Devonian: 437±12 Blankenburg Zone: Quarzit von
R4426200 H5733380 quartz–sandstone Wienrode-Altenbrak (Weller 1968);
(=Bodetal-Quarzit, Schwab et al. 1973),
Eifelian (kockelianus Zone, Fehlauer
1991)
Hg 215 Königshütte (Blankenburg Zone) Middle or Late Devonian: 422±17 Blankenburg Zone: Hüttenrode-
R4416200 H5734780 quartz–sandstone Olisthostrom (Lutzens et al. 1973),
equivalent of the Hauptquarzit? Late
Emsian? (see Blumenstengel 1973,
1974, 1975)
Hg 189 Tannenbleek near Ilsenburg Emsian: quartz–sandstone 501±10 Harzrand-Olisthostrom (Lutzens and
R4409950 H5747320 Schwab 1972), Emsian fauna (Gebhardt
1965)
Hg 216 Königshütte (Blankenburg Zone) Emsian: calcareous sandstone 412±09 Blankenburg Zone: Hüttenrode-
R4415560 H5734900 Olisthostrom (Lutzens et al. 1973),
Kalk-Grauwacke, calcareous lithic
sandstone, Early Emsian?
Hg 236 Rothäusertal near Sieber Rothäuser Grauwacke, 563±13 Blankenburg Zone: Kalk-Grauwacke,
(Harzgerode Zone) R3599150 Emsian: lithic sandstone calcareous lithic sandstone, Early Emsian
H5727500 (Erben 1953; Jahnke 1971; Weyer 1973)
Hg 235 Adlers-Berg near Sieber Devonian (?): 575±12 Blankenburg Zone or Sieber Zone?
R3598700 H5728300 quartz–sandstone
Hg 166 Klausberg, Selketal (Harzgerode Hauptquarzit, Ordovician?: 572±14 Base of Selke Unit: Südharz-Selke-
Zone) R4442900 H5727250 quartz–sandstone Quarzit, Givetian? (varcus Zone,
Ruchholz 1968)
Hg 210 Netherkpöfchen near Ordovician?: 579±12 Harzgerode Zone: Harzgerode
Güntersberge (Harzgerode quartz-sandstone Olistostrom (Lutzens and Schwab 1972),
Zone) R4429000 equivalent of the Hauptquarzit?, Late
H5723750 Emsian? (see Schriel and Stoppel 1958;
Blumenstengel 1973, 1974, 1975)
Hg 227 Präsidentenweg, Thale Late Ordovician?: diamictic 610±13 Blankenburg Zone: Harzrand-
R4432580 H5735000 sediment Olisthostrom according to Lutzens
and Schwab (1972)
Hg 225 Alte Roßtrappenstraße, Early Ordovician: 582±13 Blankenburg Zone: Harzrand-
Thale R4431900 H5735300 quartz–sandstone Olisthostrom according to Lutzens
and Schwab (1972)
Gondwana. These sediments may have derived from 2. Late Proterozoic muscovite ages could represent
Armorica during Early Devonian times. The occur- Cadomian detritus that was supplied from exhumed
rence of Lochkovian to early Emsian slates with parts of the Avalonian terrane and deposited at distal
siliceous concretions (Kieselgallenschiefer) and early shelf and base-of slope settings of Laurussia during
Emsian calcareous sandstones (Kalkgrauwacke, Early Devonian times. The Avalonian terrane, which
equivalents of the Rothäuser Grauwacke), which in- was already part of Laurussia during Devonian
clude faunal associations of Rhenish as well as times, was not detached from Gondwana until the
Bohemian elements (Groos and Jahnke 1970; Alberti Early Ordovician (Cocks 2000, 2001; Torsvik and
1995; Plusquellec and Jahnke 1999), would support Rehnström 2003). Therefore, Avalonia itself repre-
such an interpretation. Depositional units of the sents a potential Cadomian tectono-metamorphic
Rhenohercynian domain, which show affinities to source area (Winchester et al. 2002).
Armorica could give evidence of a first, soft collision 3. Similarly, Late Proterozoic muscovite ages could
between Armorica and the Avalonian part of represent recycled Cadomian detritus from Ordovi-
Laurussia during the Early Devonian (Franke and cian flysch deposits of the Danish-N German-Polish
Oncken 1995). Caledonian Belt. Greywackes of the Rügen-5 bore-170
Table 2 Revised chart of K/Ar ages of detrital muscovites from the Harz Mountains (Huckriede et al. 2004) rearranged according to the
stratigraphical age and the correct tectono-sedimentary unit
Stratigraphy of Clausthal-Kulm Acker-Bruchberg- Sieber Zone Blankenburg Tanne Zone Harzgerode Südharz-Selke-
sampled Zone (par- Zug (part of the Zone (and Zone Unit (part of
sediments authochthonous Uebernthal- northern edge the Gießen-Eastharz-
area) Gommern-Unit) of the Harz) Nappe)
Visean 376Hg152 454 Hg160
411Hg50 fl? 393Hg242 fl?
Hg51
425
Tournaisian 386Hg122 396Hg167
Hg52
Famennian 415 381Hg220
428Hg219
Frasnian
Givetian 414 Hg212 fl? 572 Hg166
fl?
Eifelian 437 Hg213
Emsian 412 Hg216 579 Hg210
fl?
422 Hg215 ›?
(501Hg189)
563 Hg236
575 Hg235 fl›?
(610 Hg227) fl?
Pragian
Lochkovian
Hg225
Ordovician ( 582 ) ›?
Cooling ages in italics indicate turbiditic flysch greywackes. Underlined ages specify revised sample assignments. Ages in brackets are from
samples of the northern edge of the Harz Mountains
hole indicate a Cadomian-influenced Peri-Gondwa- (Acker-Bruchberg-Zug) confirm Scandinavian sour-
nan detrital source (Dallmeyer et al. 1999). Exhu- ces older than the Caledonian metamorphic events
mation, erosion, and recycling of Caledonian (see Haverkamp 1991).
tectono-metamorphic source areas is reflected by the
In all cases discussed above, the co-occurrence of
Lower/Middle Devonian Old Red molasses sedi-
‘‘Cadomian’’ and ‘‘Caledonian’’ 40K/40Ar muscovite
ments (Giese and Koeppen 2001). The very low-grade
ages, which is yielded by sediments of the Blankenburg
Caledonian metamorphism only partially rejuvenated
Zone (see Table 2), argues against an Armorican origin
the argon isotopic system of the metasediments.
of the entire tectono-sedimentary unit as interpreted by
According to Dallmeyer and Takasu (1992) and
Huckriede et al. (2004).
Handler et al. (1997), detrital muscovite can retain its
Last but not least, no serious theoretical arguments
primary isotopic information up to green-schist facies
exist that can deny the occurrence of olistostroms in
metamorphism.
parts of the Harzgerode and Blankenburg Zones and
4. Late Proterozoic muscovite ages of the mica con-
along the northern edge of the Harz. Since the first
centrates probably represent pseudo-ages due to
documented examples of Reichstein (1962), a series of
mixing of different sources. Detrital material derived
stratigraphic and sedimentological case studies on out-
from Caledonian sources (440–410 Ma) and Sveco-
crops and drill cores have revealed debris-flow deposits
norwegian sources (950–800 Ma), for example, may
of various compositions (Reichstein 1965, 1970, 1991;
yield random muscovite ages between 760 Ma and
Lutzens 1972, 1973, 1978, 1979, 1991; Lutzens and
540 Ma. Relevant Sveconorwegian ages are known
Schwab 1972; Schwan 1974; Schwab 1976, 1979, 1993,
from the SW Fennoscandian Shield, particularly
1994; Stoppel 1977; Lütke 1973, 1978; Grasshoff 1983;
from SW Sweden (Johansson et al. 1991; Johansson
Buchholz et al. 1990; Hahlbeck 1990; Schust et al. 1991;
and Kullerud 1993) and Denmark (Larsen 1971,
Schwandtke et al. 1991; Wachendorf et al. 1995; Gün-
1972). They are also found in early Palaeozoic sedi-
ther and Hein 1999; Günther et al. 2001). Up to now, all
ments of the Rügen Caledonides in NE Germany
attempts have indeed failed to quantify the extent of
(Dallmeyer et al. 1999; Giese et al. 2001). Long river
resedimentation, the spatial origin of the debris flows
systems may thoroughly mix and homogenize the
and their precise stratigraphic age. The main reasons for
transported siliciclastic detritus of different sources
this are the insufficient exposure conditions as well as a
during relatively short residence times, which produce
penetrating Variscan imbrication combined with brittle
remarkably consistent apparent ages (e.g., Heller
tectonic shearing, which reshaped the olistolithes into
et al. 1992). The fact that such apparent ages are not
phacoides.
recorded from the Rheinisches Schiefergebirge can be
due to different river catchment areas. The U/Pb Acknowledgements P. Buchholz, K. Ruchholz, M. Schwab, H.
systematics of detrital zircons from early Carbonif- Weller, and H. Zellmer are thanked for providing geological
erous sandstones of the Uebernthal-Gommern-Unit background information about the areas and deposits discussed in171
the comment. Constructive reviews of H. Feldrappe and K. Obst Hahlbeck S (1990) Subaquatisch-gravitativ umgelagerte Sedimente
much improved the original script. des Devons und Karbons um Bad Lauterberg (SW-Harz). Mitt
geol Inst Univ Hannover 31:1–105
Handler R, Dallmeyer RD, Neubauer F (1997) 40Ar/39Ar ages of
detrital white mica from Upper Austroalpine units in the
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Int J Earth Sci (Geol Rundsch) (2006) 95: 176
DOI 10.1007/s00531-005-0028-8
P U BL I SH E R ’ S ER R AT U M
H. Hüneke
Palaeogeography and tectonic structure of allochthonous units in the
German part of the Rhenohercynian Belt: revision and comment
Published online: 23 August 2005
Springer-Verlag 2005
International Journal of Earth Sciences DOI: 10.1007/
s00531-005-0512-1
In the original article Table 2 was unfortunately incor-
rect. The correct version is shown here.
Table 2
Stratigraphy Clausthal- Acker-Bruchberg- Sieber Blankenburg Tanne Harzgerode Südharz-
of sampled Kulm-Zone (par- Zug (part of the Zone Zone (and Zone Zone Selke-Unit
sediments autochthonous Uebernthal- northern edge (part of the
area) Gommern-Unit) of the Harz) Gießen-
Eastharz-Nappe)
Visean 376Hg152 454Hg160 411Hg50 fl? 393Hg242 fl?
425Hg51
Tournaisian 386Hg122 396Hg167
Hg52
Famennian 415 381Hg220
428Hg219
Frasnian
Givetian 414Hg212 fl? 572Hg166 fl?
Eifelian 437Hg213
Emsian 412Hg216 579Hg210 fl?
422Hg215 ›?
(501Hg189)
563Hg236
575Hg235 fl›?
(610Hg227)fl?
Pragian
Lochkovian
Ordovician (582Hg225)›?
The online version of the original article can be found at http://
dx.doi.org/10.1007/s00531-005-0512-1
H. Hüneke (&)
Institut für Geographie und Geologie, Universität Greifswald,
Jahn-Strasse 17a, 17487 Greifswald, Germany
E-mail: hueneke@uni-greifswald.de
Tel.: +49-3834-864567
Fax: +49-3834-864572Int J Earth Sci (Geol Rundsch) (2006) 95: 176
DOI 10.1007/s00531-005-0028-8
P U BL I SH E R ’ S ER R AT U M
H. Hüneke
Palaeogeography and tectonic structure of allochthonous units in the
German part of the Rhenohercynian Belt: revision and comment
Published online: 23 August 2005
Springer-Verlag 2005
International Journal of Earth Sciences DOI: 10.1007/
s00531-005-0512-1
In the original article Table 2 was unfortunately incor-
rect. The correct version is shown here.
Table 2
Stratigraphy Clausthal- Acker-Bruchberg- Sieber Blankenburg Tanne Harzgerode Südharz-
of sampled Kulm-Zone (par- Zug (part of the Zone Zone (and Zone Zone Selke-Unit
sediments autochthonous Uebernthal- northern edge (part of the
area) Gommern-Unit) of the Harz) Gießen-
Eastharz-Nappe)
Visean 376Hg152 454Hg160 411Hg50 fl? 393Hg242 fl?
425Hg51
Tournaisian 386Hg122 396Hg167
Hg52
Famennian 415 381Hg220
428Hg219
Frasnian
Givetian 414Hg212 fl? 572Hg166 fl?
Eifelian 437Hg213
Emsian 412Hg216 579Hg210 fl?
422Hg215 ›?
(501Hg189)
563Hg236
575Hg235 fl›?
(610Hg227)fl?
Pragian
Lochkovian
Ordovician (582Hg225)›?
The online version of the original article can be found at http://
dx.doi.org/10.1007/s00531-005-0512-1
H. Hüneke (&)
Institut für Geographie und Geologie, Universität Greifswald,
Jahn-Strasse 17a, 17487 Greifswald, Germany
E-mail: hueneke@uni-greifswald.de
Tel.: +49-3834-864567
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