RUHR-UNIVERSITAT BOCHUM "'
BOCHUMER
GEOLOGISCHE UND GEOTECHNISCHE
ARBEITEN
HEn.U (1997) Bochumer geologische und geotechnische Arbeiten
Herausgegeben vom Institut fUr Geologie Ruhr-Universitat Bochum Postfach 102148 D-44780 Bochum
Verantwortliche Schriftleiter: Prof. Dr. jorg Mutterlose Dip!. Geol. Max G. E. Wippich Markus Geisen
Autoren/Auth ors: Prof. Dr. Gundolf Ernst Dr. Ursula Rehfeld Institut fUr Palaontologie Institut fUr Palaontologie Freie Universitat Berlin Freie Universitat Berlin Malteserstr. 74-100 Malteserstr. 74- 100 D- 12249 Berlin, Germany D- 12249 Berlin, Germany
Dr. Frank Horna Dr. Alastair Ruffell Geologisches lnstitut Dept. of Geology Bergakademie Freiberg School of Geosciences Bernhard-von-Cotta-Str. 2 The Queen · s University of Belfast D-09 596 Freiberg/Sachsen, Germany Belfast BT7 71NN, Northern Ireland
Prof. Dr. jorg Mutterlose Prof. Dr. Karl-Armin Troger lnstitut fU r Geologie Geologisches lnstitut Ruhr-Universitat Bochum Bergakademie Freiberg Universitatsstr. 1 SO Bernhard-von-Cotta-Str. 2 D-44801 Bochum, Germany D-09596 Freiberg/Sachsen, Germany
Dr. Birgit Niebuhr Dr. Thomas Voigt Institut fUr Palaontologie lnstitut fUr Geowissenschaften Freie Universitat Berlin Friedrich-Schiller-Universitat jena Malteserstr. 7 4- 100 Burgweg 11 D- 12249 Berlin, Germany D-07749 jena, Germany
Christopher j. Wood 20 Temple Road Croydon CRO 1 HT, Great Britain
Fi.ir den Inhalt der Beitrage sind die Autoren allein verantwortlich.
Titelbild/Cover: Das Titelbild zeigt eine nicht veroffentlichte Zeichnung des verstorbenen Franz Bettenstaedt (1909- 1978). dargestellt ist der Salzstock von Lehrte-Sarstedt zur Zeit des Santon. The cover figure is reproduced from an unpublished drawing of the late Franz Bettenstaedt ( 1909- 197 8), showing a cross section of the salt dome of Lehrte-Sarstedt in Santonian times.
Zitierweise/References: Beitrage in diesem Band sollten wie folgt zitiert werden: It is recommended that reference to this volume is made in the following form:
VoJGT, T. HoRNA, F. ( 1997): Lehofsberg near Qu edlingburg. - in: MtmERLOSE, j., M. G. E. & GE SEN , M. (Eds.). Cretaceous & WJPPICH, J Depositional Environments of NW Germany, Bochumer geol. u. geotechn. Arb., 4 6: 19-23, figs 14-16.; Bochum.
ISSN 0935-5197 Selbstverlag lnstitut fi.ir Geologie der Ruhr-Universitat Bochum Druck: Ruhr-Universitat Bochum Printed in Germany RUHR-UNIVERSITAT BOCHUM
BOCHUMER
GEOLOGISCHE UND GEOTECH HE
ARBEITEN
H EFT 46 (1997)
MUTTERLOSE, 1. M. G. E. PPICH Wl M. GEISEN (EDS.) &
CRETACEOUS DEPOSITIONAL ENVIRONMENTS OF NW GERMANY
DFG-Schwerpunkl
BIOGENE SEDIMENTATION
Bochumer geoL u. geotechn. Arb. 1997 Publication of this field guide has been made possible by generous contributions of the following organisations which is gratefully acknowledged:
Calenberg-Grubenhagensche Landschaft
Dinosaurier-Freilichtmuseum Munchehagen
Klosterkammer Hannover
Mull & Partner lngenieurgesellschaft mbH, Garbsen 3
Contents Abstract 4 Zusammenfassung 4 1. Introduction 5 (]. Mutterlose) 1.1 Lower Cretaceous 7 (]. Mutterlose) 1.2 Upper Cretaceous 13 (C. ]. Wood & G. Ernst) 2. Locality descriptions 19 2.1 Lehofsberg near Qu edlinburg 19 (T. Voigt & F. Horna) 2.2 Teufelsbachtal section near Blankenburg 23 (K.-A. Troger & F. Horna) 2.3 Hoppenstedt quarry 25 (F. Horna) 2.4 Road-cuttings near Vienenburg 29 (G. Ernst, U. Rehfeld & C. ]. Wood) 2.5 Glockenberg section 35 (]. Mutterlose) 2.6 Baddeckenstedt quarry 39 (C. ]. Wood, G. Ernst & U. Rehfeld) 2.7 Salzgitter-Salder quarry 47 (C. ]. Wood & G. Ernst) 2.8 Sohlde quarries 55 (G. Ernst & C. ]. Wood) 2.9 Gott clay-pit near Sarstedt 63 (]. Mutterlose) 2.10 HPCF 11 quarry at Misburg 77 (G. Ernst, B. Niebuhr & U. Rehfeld) 2.11 Germania IV quarry at Misburg 83 (G. Ernst, B. Niebuhr & U. Rehfeld) 2.12 Teutonia I quarry at Misburg 89 (G. Ernst, B. Niebuhr & U. Rehfeld) 2.13 Resse clay-pit 97 (]. Mutterlose) 105 2.14 Frielingen clay-pit (]. Mutterlose & A. Ruffell) 2.15 Munchehagen quarry 123 (]. Mutterlose) Acknowledgements 129 References 129 4
Abstract 15 outcrops exposing sediments of Early and Late Cretaceous age (Berriasian-Campanian) are described from the Subhercynian Basin (Quedlinburg-Blankenburg area) and the eastern part of Lower Saxony (Salzgitter-Hannover area). Apart from the bio- and lithostratigraphy, the fauna, flora, sedimentology, the palaeoenvironment and the re gional position of these outcrops is discussed. New data and results going back to re search performed from 1990 to 1996 are presented and sequence-stratigraphic models are proposed for some outcrops. Some of the microfauna and -flora and the macrofauna is documented by plates. The following outcrops exposing sediments of Early Cretaceous age are described: the Obernkirchen Sandstone (Berriasian) at Mi.inchehagen (No. 1 5), mid-Hauterivian sediments rich in ammonites near Resse (No. 13), pale-dark bedding rhythms of Late Hauterivian age near Frielingen (No. 14), Hauterivian iron ores of the Glockenberg sec tion (No. 5) and clays of Barremian and Aptian age near Sarstedt (No. 9). Outcrops of sediments of Late Cretaceous age are: Hoppenstedt (No. 3), Vienenburg (No. 4), Baddeckenstedt (No. 6), and the HPCF 11 quarry at Misburg (No. 10), exposing the Cenomanian and Lower Turonian; the sediments exposed in the Salzgitter-Salder quarry (No. 7) are of mid-Turonian to Early Coniacian age, the Lehofsberg section near Qu edlinburg (No. 1) is of mid-Coniacian age; shallow marine clastics of early Campanian age of the Subhercynian Basin are described from near Blankenburg (No. 2), marly and calcareous Campanian basinal sediments are exposed in the HPCF 11 (No. 10), Germania IV (No. 11) and Teutonia I (No. 12) quarries at Misburg.
Zusammenfassung Aus dem nordlichen Harzvorland (Raum Qu edlinburg-Blankenburg) und dem ostlichen Niedersachsen (GroE.raum Salzgitter-Hannover) werden 15 Tagesaufschli.issebeschrieb en, in denen Sedimente der Unter- und Oberkreide (Berrias-Campan) anstehen. Neben der Bio- und Lithostratigraphie, werden Fauna, Flora, Sedimentologie, das Ablagerungsmilieu und die regionalgeologische Stellung dieser Aufschli.isse dargestellt. Es werden neue Forschungsergebnisse aus den jahren 1990 bis 1996 vorgestellt und fi.ireinige Aufschli.isse werden sequenzstratigraphische Modelle diskutiert. Ein Teil der Mikrofauna und -flora sowie der Makrofauna ist auf Fototafeln dokumentiert. Der berriaszeitliche Obernkirchener Sandstein wird in einem AufschluE. in Mi.inchehagen (Nr. 15) behandelt, ammonitenreiche Sedimente des mittleren Hauterive in Resse (Nr. 13), hell-dunkel gebankte Sedimente des hoheren Hauterive in Frielingen (Nr. 14), hauterivezeitliche Tri.immereisenerze der Randfazies im Glockenberg-Profil (Nr. 5) und Tonsteine des Barreme und Apt in Sarstedt (Nr. 9). Oberkretazische Sedimente des Cenoman und tiefen Turon sind in Hoppenstedt (Nr. 3), in Vienenburg (Nr. 4), in Baddeckenstedt (Nr. 6) und in der Grube HPCF 11 in Misburg (Nr. 10) erschlossen. Das Profil Salzgitter-Salder (Nr. 7) umfaE.t das mittlere Turon bis mittlere Coniac, das Profil am Lehofsberg bei Qu edlinburg (Nr. 1) das mittlere Coniac in seiner Randfazies. Fri.ihcampanzeitliche, flachmarine Klastika des Subherzyn werden am Beispiel eines Aufschlusses bei Blankenburg (Nr. 2) beschrieben, wahrend die mergelig-kalkige Beckenfazies des Campan durch die drei Mergelgruben HPCF 11 (Nr. 10), Germania IV (Nr. 11) und Teutonia I (Nr. 12) in Misburg abgedeckt wird. 5
1. Introduction (Figs. 1-3) (by ]. Mutterlose)
In the context of the "Fifth International Cretaceous Symposium" at Freiberg from 16. 9. to 24. 9. 1996, several field trips were organized. Field trip B2 entitled "Creta ceous Depositional Environments of the Eastern Part of the NW German Basin ( Qu edlinburg-Salzgi tter-Hannover)" cov ered outcrops of Cretaceous age in the Subhercynian Basin and in Lower Saxony. The present field guide, developed from this symposium field trip, describes sec tions of both Early and Late Cretaceous age. Early Cretaceous Late From 1990 to 1996 various research D D Cretaceous projects dealing with the German Creta 1. Regional distribution of Cretaceous rocks in Fig. ceous have been funded by the German northern Germany. The area covered by this field
Science Foundation (DFG). A research pro guide is indicated. · gramme entitled "Global and Regional Proc esses of Biogenic Sedimentation" allowed rhythms, Cretaceous black shales and the fu nding of several PhD-theses covering palaeoclimatic aspects played an important palaeontologic, geologic and geochemic role within this programme. It is the objec aspects. Apart from sequence-stratigraphy, tive of this field guide to demonstrate the the analyses of sedimentary bedding results of this most recent research in the
N
0 10 A 20 30 km lehofsberg 9 Gon 1 Teufelsbachtal 10 11 23 Hoppenstedt GenmaniaHPCF IV Vienenburg 11 Teutonia I 4 Glockenberg 12 esse 5 Baddeckenstedt 13 AFrielingen 6 Salzg,ner-Salder 14 Munchehagen 7 Sohlde 15 8
2. Overview of the geographic position of the exposures described in this field guide. Fig. 6
Ei5J Upper Cretaceous D Triassic
1:::3 lower Cretaceous D Zechstein
IZZl Jurassic
0 5 10km :.. :::::::.... . · -._: _ Lehofsberg 1 Teufelsbachtal 2 Hoppenstedt Germania IV 3 V1enenburg 11 Teutonia I 4 Glockenberg 12 Resse 5 Baddeckenstedt 13 Frielingen 6 Salzginer·Salder 14 MUnchehagen 7 Sohlde 15 e
3. Generalized geologic map and the Central Lower Saxony. The sections described in this guide are Fig. indicated, for section No. see Fig. 1 14. field. Additional details are to be found in rocks in N Germany is shown in Fig. 1, the the volume "Cretaceous Biogenic Sedimen area covered by this field guide is indicated. tation and Stratigraphy" soon to be pub This guide book describes exposures from lished by Springer, synthesizing all the re three of the regions mentioned above. sults. Lehofsberg near Qu edlinburg (No. 1 ), In N Germany sediments of Cretaceous age Teufelsbachtal near Blankenburg (No. 2), occur, from west to east, in the following Hoppenstedt (No. 3), Vienenburg (No. 4) areas: and Glockenberg (No. 5) are situated in the Maastrichtian of the Aachen area, Subhercynian Basin. Baddeckenstedt (No. • Berriasian-Albian of the Emsland, 6), Salzgitter-Salder (No. 7), Sbhlde (No. 8), • Cenomanian-Campanian of the Mi.inster the HPCF (No. 10), Germania IV (No. 11) • 11 land, and Teutonia I (No. 12) quarries near Berriasian-Albian of the Teutoburger Misburg repre sent the Cenomanian • Wald and Egge Gebirge, Campanian of the the Hannover Berriasian-Hauterivian north of the Braunschweig-Salzgitter area. • Wiehengebirge, Sarstedt (No. 9), Resse (No. 13 ) Frielingen , Berriasian-Albian of the Minden (No. 14) and Mi.inchehagen (No. 15) are • Hannover-Braunschweig-Salzgitter area, exposures of the Berriasian-Albian of the Cenomanian-Campanian of the Minden-Hannover-Bra unschweig-Salzgi tter • Hannover-Braunschweig-Salzgitter area, area. Barremian-Campanian of the Sub Fig. 2 gives an overview of the geographic • hercynian Basin, position of the 15 exposures described in Maastrichtian of the Ri.igen area, this volume, Fig. 3 shows the geologic set • Cenomanian-Santonian of the Elbsand ting. The numbers used in both maps cor • steingebirge. respond to the numbers used in Chapter 2 The regional distribution of Cretaceous to describe the exposures. 7
1.1 Lower Cretaceous (Figs. 4- 11) pean area was composed of a number of (by ]. Mutterlose) basins. These formed the southernmost extension of the Boreal-Arctic sea further Overview: Marine sediments of Berriasian to the north. There also existed sea-ways Barremian age are widespread in NW Ger towards the Tethys to the south. Due to the many and, to a certain extent, in NE Eng palaeogeographic position of the NW Eu land, where they have been studied for over ropean area between the Boreal and the a hundred years. Aptian-Albian strata are Tethyan Realm, palaeoceanographic mainly exposed in southern England and changes become more obvious in this area NVV Germany. In addition, Early Cretaceous than elsewhere. Marginal epicontinental sediments are present in the North Sea area, seas like this were extremely sensitive to though the information on these is rela changes of sea-level, palaeogeography and tively scarce and patchy. palaeoclimate. During the Early Cretaceous the NW Euro- The NW German Basin, which formed the
Belemnite Bio- and litho- Ammonite Lithology STAGES zones stratigraphic zones NW NW Europe units NW Europe Germany - �- Simbirskites (C.) discofalcatus � ------I<: Simbirskites - "' Simbirskites (C.) gottschei "' Cl> z w Beds ;;; .!: 1- Hibolites -- --- '6 < -- - <:I I a; < Simbirskites (M.) staffi 'X�=�=�=�=�=�=� .0 (!) ...I jaculoides ------" ;f > Cl> capricomu l! a:: Aegocrioceras spp. (!) w - Beds - I"' Z:�-----_____ Cll 1- Endemocerasregale Cll :J _:..______:.,-:.. Cl> ------< ��:�-�-�-�-#f: - a: > Endemoceras ------:1: ...I Endemoceras noricum ·------a:: ------< Beds -- w Endemoceras amblygonium ------Acroteuthis --- acmonoides Eleniceras paucinodum Astierien Beds ------===�=�=�=��- - - Dicostella tuberculata Amoldien Beds ------Prodichotomites ivanovi �------w -:4IHII>:�------1- Dichotomites bidichotomoides -- < Acroteuthis ------z ...I Dichotomites Dichotomites triptychoides ------acre1 --=------=-- < ------Beds Dichotomites eras sus ------z - - Prodichotomites polytomus �::::::::::::------(!) Prodichotomites hollwedensis -- -- lZ:-:-:-:--=------=-:-:-: z Polyptychites sphaeroidalis - < Polyptychites ...I Polyptychites clarkei --- - < Polyptychitesmulticostatus -- > Acroteuthis Beds > ...I Polyptychites pavlowi a:: kemperi : : : < Platylenticeras involutum w ��;�� Platylenticeras : : : : : : Platylenticeras heteropleurum ---�-!IP:4i!=: -- :------Beds Platylenticeras robustum ------Peregrinoceras albidum ------I!------_____- - -- -=------=---- Surites stenomphalus ------w Acroteuthis ------1- explanatoides Surites icenii ------< ------z ...I ------�- -- < Heteroceras kochii ------I m Runctonia runctoni ---�- - <: < - - - -- ..Cl> ------Cl a:: Subcraspedites lamplughi ------.t: ------0Cl> a:: .t: -- '"<: w > Acroteuthis Subcraspedites ::; ...I Subcraspedites preplicomphalus m lateralis ...... a:: Subcraspedites sowerbyi ...... < Beds ...... w ...... Subcraspedites primitivus ......
4. Lithology and biostratigraphy ofthe Berriasianto Hauterivian interval ofNW Germany. The stratigraphic Fig. ranges of the Lower Cretaceous sections described in this field guide are indicated. 8
southernmost extension of the North Sea ate a western part (Rheine-Bentheim Basin, had a length of about 2 80 km and a Meppen-Groningen area), a central part width of about 80 km. More than 2000 m (Osnabruck-Bielefeld-Minden-Vechta area) of Lower Cretaceous sediments accumu and an eastern part ( Hannover lated in this epeirogenic basin. The central Braunschweig-Salzgitter area) (ScHorret al. partsof the basin are characterized by con 1967, 1969). The sections described in this tinuous subsidence and great thicknesses field guide are situated in the eastern part of shales and mudstones (Figs. 4, 5). Along of the basin. Detailed descriptions of the the margins, however, shallow water evolution of the basin have been given by sediments including sand- and ironstones SCHOTI et al. (1967, 1969), MICHAEL (1974, were deposited. Due to lithologic variation 1979), KEMPER (1979) and MUTIERLOSE (1992). within the basin, it is possible to differenti- This field guide aims to demonstrate the
Belemnite Bio- and litho- Ammonite Lithology zones stratigraphic zones NW STAGES NW-Europe units NW-Europe Germany
Neohibolites w praeultimus
Neohibolites 5 _ oxycaudatus Dipoloceras cristatum ______...... z Euhoplites lautus ...... cc w ...... I t---M-:-�:-:-�:-:-:-:-�-:s"_P:-,�-m----t1�1�1�1�ltlt------�...... Q minimus Neohibolites uhoplites loricatus m Q Beds E : : :: ...I minimus : : : : :i •••••••• cc t------+Hoplites dentatus ::::::::
f-- t------�-...... - ... Douvil/eiceras mammillatum - t------(_-� - - -- > Neohibolites - -- ...I Leymeriella regularis minor � a: Leymeriella tardefurcata � t-N- e -oh- ib- o -lit -es--f --:-:-:-:��- . ...- :-:-. strombecki Proleymeriella schrammeni ...... 1-- H- -P - - - t------bt . Neohibolites jacobi no/ani - -- � _ wollemanni Clay 1 , :::::::::::::a: -i�:�������� w t-���-�----r�------�------� Neoh olites ib fl M rt i !;;;( in exus a Parahoplites nutfieldiensis :: :: ::: : •••••••• ...I t-�m�ffe�x�u�s-�---��t------rNeohibolites jj Epicheloniceras tschemyschewi :::::::: z clava Marl � -c:_la_v _a_ --- Qj cc� 1-- -+ ---1 .c., Tropaeum drewi :::::::: c .c� ., f-- ewaldi :::::::: .>: "C ...... u A. M :J!_ Tropaeum bowerbanki 0 Neohibolites art � � � � � � � � C3 CC ewaldi > Fischschiefer � ...I s a: cc o�!����:!f - � w � � � � � �- �- r------;------t----���----��:������bodei - - Prodeshayesites ------Clay tenuicostatus t�-�-�� -�-�� Oxyteuthis �------�------{�-::=��-:= depressa depressa Parancyloceras bidentatum Clay t------e=;;;=���=��� t-----+------1 Simancy/oceras stolleyi ------t------+==�:-:::::: w Oxyteuthis - - -- Ancy/oceras innexum - - germanica ------Oxyteuthis ------5 Beds t------t=-�_;;_��� Parancyloceras denckmanni ------Oxyteuthis t------t�::::::::----- brunsvicensis ------
- Praeoxyteuthis Chondrites --- - Beds ------pugio Hoplocrioceras rarocinctum =--�------=-
5. Lithology and biostratigraphy of the Barremian to Albian interval of NW Germany. The stratigraphic Fig. ranges of the Lower Cretaceous sections described in this field guide are indicated. 9
Barremian Fenno - Berrlaalan Fenno Scandta -NOfl·rnanrleWulden Scandia - NOI'I-marme Wealden OPre5Ul'T'I8'CILanc:l D•-land •o...o ....Tethyan1nhu1 •o...o ....T hyan�nllu• ..
• EDINBUI'lG>o
Anglia Anglia
/ / .Bt... � • Allrr'E ...... -� Rheno - Aheno - Bohemi a Bohemia �,... �
Mo>C>< • PAll!$ Tethys Tethys ·M�ICH
6. Palaeogeographic setting of the Berriasien of 8. Palaeogeographic setting of the Barremian of Fig. Fig. NW Europe. NW Europe. palaeoceanographic changes occurring many (Figs. 7, 10). These are represented within the Early Cretaceous of NW Europe by the fully marine Plarylenticeras Beds. by integrating sedimentologic and During the Early Valanginian transgression, palaeontologic observations. The distribu the Carpathian sea-way opened towards the tion of sediments and biota clearly reflect Tethys via Poland. This sea-way, which ex palaeoceanographic changes throughout isted throughout the Valanginian, enabled the Early Cretaceous. These data are based an exchange of Tethyan and Boreal on most recent studies of the lithology, nannofloras and faunas. The Gifhorn Chan geochemistry and palaeoecology of the nel, the Hoya Channel and the Ems Chan Berriasian-Albian interval. nel linked the NW German Basin to the southern North Sea via the Pompeckj Block. Evolution of the NW German Basin: The marine floras and faunas of the Early The Berriasian is represented by non-ma Valanginian of NW Germany have a Boreal rine Wealden sediments, deposited under character, Tethyan elements being largely brackish-lacustrine conditions (Figs. 6, 10). absent from the Boreal Realm at this time. However, several short-lived marine incur A widespread transgression is evident for sions occurred, allowing marine biota (in the early Late Valanginian over much of cluding foraminifera) to spread into the Europe. This caused an expansion of the basin from the northwest via the Nether NW German Basin, in many places Late lands. The base of the Valanginian is Valanginian sediments rest with a non-se marked by a major transgression and the quence on Berriasian strata. In the western return of marine conditions in NW Ger- part of the basin the Lower Valanginian
Fenno · Fenno • Aptian V•illnolnllinNor'l-manroe -MIIuterivlanWealden -N00'1 fnllr>niiWUIOen Scandta Ill Scandi a · 0 P•esumecllencl DPresumea rw:� ..
.eo......
Angl1a Anglia
/ / •WAM.Aw / / •BEAL .. ---/ •....,., • -- .-"" ,...... ,_ / ...... _ / Rheno Rheno · / Bohemia Bohemia ...... Armor1ca Armortca �� Tethys Tethys . .. __ 7. Palaeogeographic setting of the Valanginian Palaeogeographic setting of the Aptian of NW Fig. Fig. 9. Hauterivian of NW Europe. Europe. 10
"' Ql "' >. Qj Calcareous c >.� > STAGE Lithology Benthos Cephalopods ·n; m- Ql nannofossils E 3: Ql eo 0 m 1- Ql 0 (J)_
Polyptychites 8 ------M. t--+---t-:-:-:-:-:-:-:-:-- - : :-:-:-:-:-:-:-:-: speetonensis Platylenticeras =�:------Q) ------S. arcuatus Surites c;; ------�GB--��P. fletcheri Acroteuthis ...J
10. Distributions of nannofloras and faunas, sea-ways and assumed sea-level curve for the Berriasian Fig. Hauterivian intervalin NW Europe (modified after MurrERLOSE 1992). Sea-level curveaccording to observations in NW Europe.
Bentheim Sandstone is overlain by clays. Valanginian ( =Astierien- and Arnoldien The mid-Late Valanginian Dichotomiten Beds), there were extensive influxes of both Sandstone of NW Germany may record a Tethyan nannofloras and faunas via the subsequent minor regression, followed by Carpathian sea-way (Fig. 7). the transgressive Arnoldien- and Astierien For the Hauterivian, the general outline of Beds. Overall, Boreal nannofloras and fau the palaeogeography is similar to that of nas dominate most of the Late Valanginian the Valanginian. In NW Germany marine of NW Europe. During two periods, in the strata of Hauterivian age are widespread early Late Valanginian and in the latest and, in the basin facies, they are repre- 11
Plankton
Lithology Benthos Cephalo ods STAGE Calcareous forams p nannofossils rads +
'* ======�:=:=:=:=:=:=�=::
...... Neohibolites ...... � ...... �������� ...... ����� forams: c high divers. c:: cosmopolitan Q) assemblages a. Neohibolites 0 ------Q) ------minim us c:: c:: CO .c (.)I forams: .9 low divers. e a. �----- Neohibolites B �---- AucellinaBuchia corals T R. .1...1...... Nuculana ...... Nannoconus Toucasiaforams: Duvalia c _ ro � � : asper high divers. Zurcherella / c I � : : : : : : 0. Neohibolites I <:{ Prediscosphaera Tropaeum T Duvalia c ------F. Neohibolites - R. ------T -t-:... -:_-_-_-_-_-_-_-_ C. 1--+- biforaminis comm irregularislitterarius t Q) - - ______--- _ _ _ _ _ -----_ _ _ Oxyteuthis n; � Hedb. -- c - ---_ _-_-_-_-_-_ Z. sisyphus _ _ _ _ _ CO _----_-_-� N. borealis ------· N. abundans Aconeceras .EQ) :=:=:=:=:=:=:=:=::: - E ...... CO Oxyteuthis CD Aulacoteuthis
---:-E:S-:------N. abundans Fig. 11. Distributions of nannofloras and faunas, sea-ways and assumedPraeoxyteuthis sea-level curve for the Barremian Aptian interval in NW Europe (modified after MurrERLOSE 1992). Sea-level curve according to observations in NW Europe. sented by more than 400 m of clays. In the Endemoceras amblygonium ammonite marginal areas, thicknesses are reduced Zone. The Grenz Sandstone at the and the clay is partly replaced by Valanginian/Hauterivian boundary in NW sandstones or ironstones. Early in the Germany records a minor regression within Hauterivian a major transgression further this transgressive sequence. A subsequent expanded the NW German Basin (Fig. 7). regression of late Early Hauterivian age is This transgression began in the latest marked by the norcium Sandstone. The lat Valanginian (Arnoldien Beds) and reached est Valanginian (Arnoldien- and Astierien its maximum in the Early Hauterivian Beds) and the earliest Hauterivian are char- 12
acterized by a strong influx of Tethyan creases. These sediments are enriched in nannofloras and faunas, which must have organic matter ( 6 to 8% TOC) and were used the Carpathian sea-way. The regres deposited under anoxic conditions. The sion of the late Early Hauterivian Barremian was a period of restricted con (Endemoceras regale ammonite Zone) was ditions, allowing the deposition of these followed by an extensive mid-Hauterivian organic-rich sediments. The transgression (Aegocrioceras ammonite palaeogeographic and palaeoceanographic Beds and lower Simbirskites (M.) staffiam configuration favoured the evolution of monite Zone). After a regression in the mid endemic species from Tethyan ancestors at Late Hauterivian (upperS. (M.) staffi am the Hauterivian/Barremian boundary. Simbirskites gottschei monite Zone and (C.) Within both nannofloras and faunas, en ammonite Zone), recorded by the Gildehaus demic species evolved simultaneously and Sandstone, another transgressive peak is to became quite abundant. These are associ be observed in the latest Hauterivian ated with Boreal elements, while Tethyan (Simbirskites discofalcatus (C.) ammonite forms are extremely rare or absent. Zone). Several transgressions, with intervals of Nannoflorasand microfaunas of low diver shallowing and regression in between, sity and abundance are present in the through the Aptian and Albianenlarged the lowermost Upper Hauterivian depositional areas in NW Europe (Figs. 9, ( =Aegocrioceras Beds), the ammonites be 11). The Early Aptian transgression caused ing of Boreal, Tethyan and endemic prov significant changes in the palaeogeography. enance. This level correlates with the wide New sea-ways between the Tethys and the spread mid-Hauterivian transgression. The Boreal Realm opened via northern France middle pan of the Upper Hauterivian yields and southern England, while brackish Boreal and endemic nannofloras and fau lacustrine deposition prevailed in Poland. nas, with brief influxes of Tethyan ammo In NW Germany, the Aptian comprises at nites ( Crioceratites). The biota indicate a least 200 m of clays and marls. Dark clays regressive phase, Tethyan nannoconids ( bodei Clay) are overlain by the being absent from this interval. Finally, Fischschiefer, a finely laminated sediment Tethyan influxes of nannofloras and fau rich in organic matter (Figs. 5, 11). Above nas again become obvious in the uppermost this horizon follow dark clays and three Hauterivian. This is supported by recent marly horizons rich in carbonate: the finds of foraminifera of warm water affini ewaldi Marl, the clava Marl and the inflexus ties and bryozoans in the discofalcatus Marl. The uppermost Aptian consists of Zone. dark clays. Cosmopolitan elements domi Significant palaeogeographic and nated in NWEurope and the endemic forms palaeoceanographic changes occurred at of the Barremian became extinct. The fluc the Hauterivian/Barremian boundary; the tuations of the calcareous nannofossils, in overall regressive nature of the Barremian particularthe distribution of nannoconids, is often cited. A regression at the base of indicate three periods of Tethyan influxes: the Barremian caused brackish-lacustrine 1) lowermost Aptian, 2) ewaldi Marl, 3) conditions in central and southern Poland. inflexus Marl. On the other hand, three In NW Germany, the entire Barremian periods without or with only few reaches a thickness of more than 200 m. nannoconids can be recognized: 1 ) black The sediments, nannofloras and faunas in clays below the Fischschiefer, 2) the clava both areas are uniform throughout. Finely Marl, 3) the black nolani-jacobi Clays. laminated sediments, known as "Blatterton" Sediments of earliest Albian age resemble horizons, are typical of the Barremian of the black nolani-jacobi Clays. It is only in NW Germany (Figs. 8, 9). While the the mid Early Albian and mid-Albian that "Hauptblatterton" (main Blatterton) is of a major transgression changes the late Early Barremian age, thin Blatterton depositional environment significantly. horizons are common in the early Late Barremian. Towards the centre of the ba References: KEMPER (1979); MICHAEL (1974, sin the number of Blatterton horizons in- 1979); MuTTERLOSE (1992 ); ScHoTT et al. (1967, 1969). 13
1.2 Upper Cretaceous (Figs. 12, 13) SSW) Harz northern boundary thrust, the (by C. ]. Wood & G. Ernst) Upper Cretaceous (Cenomanian-Lower Campanian) attains considerable thick Overview: The localities to be described nesses, locally more than 2000 m. This is belong to the eastern sub-basin of the the classic example of sedimentation in a Hercynian (WNW-ESE) trending Lower subsiding marginal trough in front of an Saxony Basin (LSB), i.e. the area E of the inverting massif (VoiGT 1963 ). During the NNW-SSE Steinhude Lineament (BALDSCHUHN early part of the Late Cretaceous, the sea et al. 1991 ). The LSB graben underwent actually extended far to the south and the subsidence from early Portlandian to late area occupied today by the Harz formed Aptian times, after which there was reduced part of the original basin. The discovery in tectonic activity until the late Turonian. the Cenomanian at Baddeckenstedt, ea. 35 Inversion began in the early Coniacian, km from the Harz, of a group of gastroliths reached its peak during the Santonian and comprising lithologies of probable Harz continued into Campanian times. Further massif provenance suggests that at least inversion took place in the latest Cretaceous part of the massif must have been emer and early Tertiary. The cumulative inver gent as an island at this time (ERNST et al. sion converted the former graben into the 1996). However, following uplift, the mas present tectonically stable Lower Saxony sif formed the coastline of the Cretaceous tectogene. sea, as demonstrated by the occurrence of Since Upper Cretaceous deposition in the marginal facies. area and the extent to which the sediments In the northern synclines, the Upper Cre have been subsequently preserved are taceous is much thinner and includes larger strongly controlled by the structural set sedimentary hiatuses resulting from ting, it is necessary to describe this aspect Subhercynian tectonism. In the Beiwende before considering the stratigraphy. Three Syncline, S of the Asse Anticline, higher major structural units can be distinguished, Santonian or Lower Campanian rests on comprising, from E to W: 1) the Hercynian Middle Turonian, while in the trending Subhercynian Basin, 2) the Schoppenstedt Syncline to the N, the Up Rhenish zone, 3) the Hercynian zone S and per Cretaceous succession ends low in the W of Hannover. Turonian. In the Beienrode Basin, Creta ceous sedimentation began with the latest The Subhercynian Basin (SHB): The Early Campanian mucronata transgression: SHB is bounded to the SW by the Harz block here glauconitic sediments rest on Middle and to the NE by the Flechtingen High. It is Keuper (NIEBUHR & ERNST 1991 ). diffe re ntiated into a succession of Uplift of the Harz massif during the late Hercynian-trending broad symmetrical salt Cretaceous resulted in steeply inclined to pillows (Fallstein and Elm) and narrow overturned ( 85° SSW) Mesozoic strata in the asymmetrical, salt-injected anticlines narrow zone ("Aufrichtungszone") paral (Harli-Berg or Vienenburg and Asse). Re lel to the northern boundary thrust. There flection seismic work (BRONING et al. 1987) were two main (so-called "Subhercynian") has shown that the Harli-Berg Anticline, like inversion phases, the Ilsede and the Qu edlinburg Anticline, is a salt-injected Wernigerode Phases, the latter being struc thrust structure resulting from inversion turally the more significant. Each uplift of the Fallstein. The Asse and Elm form an phase was followed by a phase of renewed analogous structural pair. The SSW-directed transgression, so that in the Harli-Berg thrustopposes the NNW-directed Aufrichtungszone there is repeated onlap Harz northern boundary thrust. The Dorm of later strata over the earlier upturned Anticline is a narrow salt structure with strata. The Subhercynian inversion phases diapirs. The Upper Cretaceous is preserved (tectoevents) are expressed in the sedimen in the interveningsynclines (Subhercynian tary record by significant lithofacies Cretaceous Syncline, Beiwende Syncline, changes (e.g the change from Planer car Schoppenstedt Syncline and the Beienrode bonate facies to Emscher argillaceous Basin) either as largely complete facies) and/or major hiatuses. They also successions or as isolated relicts. In the caused or accentuated uplift of pre-exist Subhercynian Cretaceous Syncline, situated ing salt structures throughout the area, cre parallel to the steeply inclined (40°-50° ating submarine swells or even island 14
chains, with resultant fades differentiation There is an area of structural complexity N of Cretaceous sedimentation. To varying of the Harz where three major structures degrees, the effects of these phases can also intersect. The Rhenish Wendeburg fault be recognized throughout Europe. zone with the Broistedt salt structure at its The onset of the Ilsede Phase is seen in southern end comes into juxtaposition with Vienenburg (No. 4), where Early Coniacian the oblique-Hercynian (NNW-SSE), salt-in mart-limestone alternations with jected, Salzgitter Anticline and the adjacent inoceramids are interrupted by glauconitic E-W Lichtenberg-Hohenassel structure , turbidites. The Wernigerode Phase can be both of which are northward-directed accurately dated to within a single asymmetrical inversion structures. Move macrofossil zone, indicating very rapid ment of these structures and uplift of the uplift: in the Subhercynian Syncline, late salt structure controlled sedimentation in Santonian Heimburg Beds rest discordantly the area to the N (Lesse Syncline). Here, on the Teufelsmauer Sandstone, both yield the subsequently steeply uptilted thick ing Marsupites (VoiGT 1929). limestone-mar! successions (Salder quarry; No. 7) developed in the foredeep or mar The zone of Rhenish structures: The ginal trough between the salt structure and SHB is truncated to the W by a zone of the invertingLichtenberg structurecontrast Rhenish (NNE-SSW) structures, which fol with thinner, chalk facies successions lows the Rhine Graben-Gifhorn Trough (Sohlde quarry; No. 8) deposited on the Lineament (see NIEBUHR 1995 ). This zone shelf only a few kilometres away on the N strongly overprints the Hercynian struc flank of the syncline. These quarries and tural trend and includes most of the area the Baddeckenstedt quarry (No. 6; between Braunschweig and Hannover. It is Cenomanian-Middle Turonian) in the characterized by several subparallel elon Innerste Syncline to the S will be described gate Rhenish salt structuresassociated with below. complex fault-zones, which represent a con The Santonian iron-ores formerly worked tinuation of the swarms of similar struc in the Gro.&-Ilsede area and near Broistedt tures to the north. These salt structures represent the marginal basal conglomerates comprise, from E to W, the Broistedt salt of a Santonian transgression following the structure, the salt structures in the Subhercynian Ilsede tectoevent and uplift Stederdorf Graben, the Lehrte-Sarstedt salt phase. The conglomerates, which are com structure and the Benthe salt structure (Fig. posed of ironstone geodes and phosphates 54). reworked from the Albian, rest with ero The Upper Cretaceous is preserved on the sive contact either on Albian (Gro.&-Ilsede) flanks of the salt structures and in the in or Middle Turonian (Broistedt), in each case tervening broad synclines (Meine-, Peine-, in proximity to a salt structure. It is this Lehrte West- and Pattensen Synclines). major hiatus at Gro.&-Ilsede that gives its Typically, only the higher stages name to the first Subhercynian uplift phase (Santonian-Campanian or just Campanian) and its associated regression. NIEBUHR 1995). are found here ( However, in the Kronsberg Syncline adjacent to the Zone of Hercynian structures: S and Lehrte West Syncline, as well as in the W of Hannover, the Rhenish zone abuts Pattensen Syncline, Cenomanian and Lower against a zone dominated again by Turonian are preserved beneath transgres Hercynian structures. The main occur sive Santonian, most of the Turonian and rences of Upper Cretaceous are in the Hils all the Coniacian being missing as a result Syncline (Cenomanian), Sack Syncline of the Ilsede tectoevent. The thickest and (Cenomanian-basal Coniacian), Wunstorf most complete Campanian successions are Cretaceous Syncline (Cenomanian found in the Lehrte West Syncline, where Turonian in the Wunstorf quarry) and the several quarries (Hover, Misburg; Nos. 11, Gehrden Graben. In the graben, Santonian 12) and gas pipeline sections (Ahlten) have calcarenites with a basal ironstone con provided a composite section up to the glomerate rest on Barremian to Aptian higher part of the Upper Campanian. A mudstones. small tectonic unit of Upper Maastrichtian is preserved as field brash at Ilten to the E Stratigraphy: The stratigraphic diagrams of these sections (VoiGT 1951 ). (Figs. 12, 13) are intended to be largely 15
1 2 No 3 No No 10 11 12 -�, No No No 4 No 6 7 8 No No I No
Bkwlrwtlon
i. '•"Qf!f �1------J ..0:: "E .. CL E 1--+-----� .. u... CL.. CL ::1
SIObaellbiJStp lana
? •
subqu•dfltus
?
?
.'"um -'-sl1m" '.", l---- g o � � _ _ _n go_n g uora ---l :i f--+---
·· ·· "' 0 : f---__----1 "lll§l.§ mantelh�
12. Stratigraphic ranges of the described Upper Cretaceous sections. Fig.
(ERNST 1983 self-explanatory, to avoid duplication of in various types et al. ), was origi formation given under the descriptions of nally developed in this area and the com the localities. The event stratigraphic ponent events are documented in greater scheme for the Cenomanian-Coniacian suc detail elsewhere in this guide. It is now cession, which comprises over 30 events of known that some of the events first tenta- 16
Eustaticand tectoevents of the Northem German shelf basin 65 (transgressions and r.gressions) (tectoevents)
c CD ea 0 ;::: juniortr. >-0 s:.CJ .!!!c "i: E 70 0 ... ·;:: 11) ea ;;; ea (IJ � (IJ ::::!;
Oebisfelde tr.
75 c po/yp/ocumre. (IJ li)C.,c.<�� c.C.>. o ::::�Eo (IJ u mucronata tr. '- 80 ci GJ Peine te. �Eo � O tll>- o pilula tr. -'U
c (IJ : subhercyn. Late Santonian ·c:� tr. 0 0 Wemige- - >-0 li l rode te. 85 Middle ntonian tr. en 10 Sa G :>� > .!! Emscherian tr. � subhercyn. Hyphantoceras .Eisedete.� lr. costellatus/plana tr. hercynicus Turonian 90 Mytiloides tr. te. tr. � plenus/denisonianum tr. Late Ceno- manian te. Pycnodonte/jukesbrownei tr. �
primus lr. 95 Early Cenomanian tr. = ultimus/Aucellina tr.
limestone D chalk Y glauconite black shale marl conglomerate, residual iron ore L;;iiil quartz detritic calcarenite ----- marly clay and shale • red coloured carbonate R D hiatus opoka (spiculitic marl) F fluvial-deltaic deposit • 'Q' Fig. 13. Upper Cretaceous lithofacies, eustatic and tectonic events of the North German Basin (after NJEBUHR & PROKOPH in press). tively identified here are of inter-regional The Planerkalk can be further subdivided lateral extent. The generalized into five lithological subunits. Beginning lithostratigraphic succession is shown with a basal transgression, marked by graphically in Fig. 13. Four major litho glauconitic marls with phosphatized peb units can be recognized as follows: 1) the bles (seen in the Floteberg road-cutting), Planerkalk (Cenomanian-Lower Coniacian), the Cenomanian is developed as initially 2) the Emscher Marl (Lower Coniacian argillaceous (Cenoman-Mergel) and later lower Lower Campanian), 3) the Mergelkalk increasingly calcareous sediments (upper Lower Campanian-lower Upper (Cenoman-Kalk). There is a major facies Campanian), 4) the spongiolitic "Opoka" change near the top of the Cenomanian facies (upper Upper Campanian). Above the from white, pure limestones to variegated last unit, calcarenites of early Maastrichtian argillaceous sediments. These are devel age are known from deep boreholes to the oped as thin successions of red limestones N of the area. and marls (the so-called "Rotplaner" facies) 17
in the oxygenated environments over swells Subhercynian Ilsede tectonism and salt and platforms, while in the adjoining ba movement, the Emscher Marl facies begins sins are found thick successions of organic even later, with the post-Wernigerode carbon-rich dark grey mads alternating tectoevent Marsupites transgression, e.g. with very pale limestones, constituting the near Misburg. Here, Turonian Planer is Black Shale or "SchwarzweiB,e overlain by a glauconitic mad with abun Wechselfolge" facies. The latter represents dant Gonioteuthis. the Oceanic Anoxic Event 11 in the The overlying Mergelkalk comprises incon Cenomanian/Turonian boundary succes spicuously developed argillaceous mad sion. limestone alternations with, locally, a ba The Black Shales end in the Lower Turonian, sal glauconitic transgression horizon en but the RotpHiner continues to near the top riched in Gonioteuthis marking the pilula of the Middle Turonian. These units are fol transgression. Reflecting the polyplocum lowed by the WeiB,planer, developed as regression eustatic event, the mad-lime argillaceous limestones in basins and as stone alternations are replaced upwards by chalk facies over swells. The WeiB,planer spongiferous, spiculitic m ads ( "Opoka" includes several vulcanogenic mads (tuffs), facies) with a rich fauna dominated by large which constitute isochronous tephroevents oysters, together with and moulds of that have been used to correlate Turonian aragonitic bivalves and gastropods (NIEBUHR successions throughout Germany. The thick 1995, 1996a). ME marl-seam used here as a datum-plane In the Peine Syncline and elsewhere, a fur can even be traced to northern England. ther tectoevent, the Peine Phase (RIEDEL The WeiB,planer is succeeded by the 1940) and subsequent mucronata trans GrauweiB,e Wechselfolge, which is charac gression, is found near the top of the Lower terized by laterally correlatable conspicu Campanian. ous limestone-mad alternations of uncer In the Beienrode Basin, the Cretaceous suc tain origin and includes the Turonian/ cession begins with the mucronata trans Coniacian boundary event-bundle (Fig. 31 ). gression. Here the lower Upper Campanian The top of this unit is marked by the llsede is developed in marginal glauconitic facies, tectoevent, which is reflected by a major with the polyplocum regression being fa cies change from carbonates to the marked by a change to continental quartz argillaceous and somewhat monotonous sands which continue into the Upper
Emscher Marl. Maastrichtian (NIEBUHR & ERNST 1991 ) . The ln the basinal areas, the marl facies contin Ilten Maastrichtian occurrence (VoiGT 1951) ues into the Lower Campanian and there is with its basal conglomerate marks the Up little evidence of the pre-Hercynian inver per Maastrichtian junior transgression: in sion phases. In some marginal areas (GroB, the Beienrode Basin, this event is suggested Ilsede, Broistedt, Gehrden), the (post-Ilsede) by increasing indications of marine influ transgressive Lower to Middle Santonian ence towards the top of the continental develops a ferruginous basal conglomerate. quartz sands. The overlying beds are calcarenitic and highly fossiliferous, yielding a fauna (par Refe rences: BALDSCHUHN et al. (1991); ticularly echinoids) that is totally different BRONING et al. (1987); ERNST (1968); ERNST et from that of the correlative marl facies (ref al. (1983, 1996); NIEBUHR & ERNST (1991); erences in ERNST 1968). In other areas that NIEBUHR (1995, 1996); RIEDEL (1940); VoiGT have been uplifted as a result of (1929, 1951, 1963). 19
2. Locality descriptions Emscher Marl rests unconformably on Mid 2. 1 Lehofsberg near Qu edlinburg dle Turonian or Upper Turonian coccolith (Figs. 14-16) limestones. This unconformity is inferred (by T. Voigt & F. Horna) to be connected with activity of the Qu edlinburg salt structure (VoiGT 1929; Location and grid reference: TK 25, TROGER & ULBRICH 1971 ), or it may be the 4133 Wegeleben, R: 4442250, H: 5742 150. expression of the marginal position of these The Lehofsberg sections, an abandoned and localities (northeastern basin margin). a working sand pit, are situated 2 km north The overlying Formsand Formation (Unit of Qu edlinburg by the old road to Ditfurt 3) marks the beginning of sand (Figs. 2, 14). pro gradation from the northeast (demon strated by the granulometry), a sedimen Tectonic setting: Southern flank of the tation pattern which persisted from the Halberstadt Syncline (Fig. 14). This NW-SE mid-Coniacian to the Late Santonian. structure is 4.5 km wide and about 14 km Volviceramus koeneni , In oceramus long. sublabiatus, I. kleini and I. percostatus and members of the Pla tyceramus mantelli Coniacian: The Coniacian of the group establish the early mid-Coniacian age Subhercynian Basin is divided into 5 units. of the silty, fine-grained sands. The Lower Coniacian (Unit 1) consists of The top part of Unit 3 is characterized by an alternation of marls and limestones-the increasing glauconite content, which con so-called "Grauwei�e Wechselfolge" -yield tinues in the overlying Unit 4 (involutus Cremnoceramus ro tundatus , erectus ing C. Sandstone Formation). The distinct coars and C. crassus. ening upward trend is expressed by a tran Unit 1 is overlain by the Emscher Marl For sition from fine- to medium-grained mation (Unit 2), which consists of homo sandstones with siliceous cementation. geneous marls and silty marlstones with Common cross-bedding and increasing common glauconite at the base. In the east density of event-beds (probably storm-lay ern part of the basin a stratigraphic gap of ers) indicate a change from a lower considerable duration is developed: the shoreface environment to a current-influ Grauwei�e Wechselfolge is missing, and the enced setting. Unfortunately, the high en-
Stratigraphy and Lithology
Coniacian to L. U. � Santonian: sands!., � days and mar1s
M. Coniacian: lnvolutus � sandstones L...... _l 5 km M. Coniacian: glauconitic � sandstones L.:.=:J L. Coniacian to L. Santonian: � Emscher Mans L..:....:.J Cenomanian to Low. Coniacian: c:::I:lJ l1mestones and marls a:::IJ Lower Cretaceous (? Hauterivian � to Aptian): sandstones L.:.=:J Jurassic (Lias): day, sandstones, � limestones and Fe-oolites E2H Triassic (Keuper): clay, mar1s. sand � stones, dolomites and gypsum � Triassic (Muschelkalk): limestones. D.2..IJc::::I::II mans, day and gypsum
14. Geologic sketch map of the Halberstadt Syncline (after TRbGER & KuRzE 1980). Fig. 20
Age Zilly-Benzingerode (W) Quedlinburg (E) Pebbles of phosphorite and coccolith lime stones within the involutus Sandstone are
<:: particularly important.They reflect rework "' c ing of Cenomanian and/or Turonian depos Qj�E � its in the source area 1929). 0"' ...J l) � nkenburg (VorGT Formation The late Coniacian is represented by the ? � 5) . E., �� He1mburc Formation Munchenhof Sand Formation (Unit u I <:: Heidelbergsandstone Member which consists of fine-grained sandstones ·"'c: .E � reflecting the transition to marl sedimen m - Salzberg Formation "'c !!l � tation in the southeastern part of the en - Eio I Milnchenhofsand Subhercynian Basin. These marls yield Formation ?- Magadiceramus subquadra tus which indi <:: -u ·r;"' cates a late Coniacian age. "' --- � sandstone Format1on c m Ill lnvolutus 0 � l) E t Formsand Formation Stratigraphy and lithology: The locali � ties west of Qu edlinburg expose middle 15. Lithostratigraphic scheme of the higher Up Fig. involutus per Cretaceous in the eastern Subhercvnian basin. Coniacian sandstones ( Sandstone; (after TIWARI & 1973 ). Figs. 15, 16). These sandstones are com Rm, posed of quartz which was probably de ergy also prevented the preservation- of rived from Buntsandstein (Triassic) and fossils, so that it is difficult to place exactly Early Cretaceous sandstones. This prov the biostratigraphic boundary between the enance is inferred from the high maturity zone of V. koeneni and the overlying zone of the heavy mineral association. Further of V. in volutus, which has been recognized more, the quartz surfaces and present rel at some localities in the up to 50 m thick ict cements indicate a fluvial environment. succession. In the large sand pit south of Lehofsberg, the transition from greenish, clay-rich
c � c 0-o "' �·"' c � Q c: Q �= ;;; 6J c " • .!! C1lg� Ill� � '0 G.'-�� � - - c E 0-"' E � E� u Q. � §.� � -& E :!{ E �� "' • �.c... ::;� •.c Cl; 2! 'g ;; e- .. � Uthology c, - _c .. ' �0. .!!! . traces.'m" E • [g -o ;;, u 20 m!!,....,..,,..,.....,..,.,.,_.,...., � 0,25 1 0 -40 4 3 2 I 0 0- s,2 c I I I I Ill 'PS! I N - Ill l � � I i ! I "0 E mass•ve mediU'TI- to coarse-gramed r I f � c w1th channelS "' av. sandston� •nle•calated '<:::___./ subhonzontal lam1nat•on and ;;:: 1: coar sa"ld laye· c. "' <:: ·�d•shncl se s I (/) -c "' :J � ! N Cl t'm.uon �ur(oc(' ·-<:: - ;;:: 0 masstve to th•ck-bedded med1Jm-gra1ned � sand yellowish-grey cross-bedded N "' 1/) channe•s W11h norrnall'ol graded c .r:. coshallowarse-gra1ned san:::l � � Ill :; - u I - "0� n; I ' ' & "' ] N I I ;;:: I c. I :J
I Cl I ·-<:: 6)N Q) <:: u P3 I Q) � i I 1/)� greenish-brown. glaucond1c hnesand. :\I � 0 slrong'y �p "' .r:. b10turbated I P2 I cg 0 1/) .....,;.....,...-..__.,1 lmrnmtu· hor�:on u iii grey-greenish. glaucon•trc hne-gra1ned sand. ;;:: massrve (homgeneously b1oturtate:l) P1 ___ ? I .2 Om_._ ....l ' 11 II 16. Lithology and sedimentologic patterns of the Middle Coniacian of the Lehofsberg sand-pit. Fig. w 21 sandstones to medium-grained cross-bed glomerate beds, up to 0.4 m thick, consist ded sandstones is accompanied by increas of well-rounded quartz pebbles. They be ing grain size and decreasing glauconite come more closely spaced and thicker up content. Fossils are very rare, only some section and are interpreted as proximal bivalve fragments including Volviceramus tempestites. involutus have been reported from the sandstones. The upper parts of the succes Heavy-mineral assemblage (after sion fo rm a steep rock massif which is trace Tiwari & Roy 1973): able around the Halberstadt Syncline, com zircon: 77% (sedimentary >> magmatic), • posed of thick-bedded sandstones. In the tourmaline: 11%, • lower part of this unit, silty and marly rutile: 6%, • interbeds with rippled surfaces, mud others (staurolite, kyanite, garnet, • drapes and graded bedding may indicate pyroxene.. . ): 6%. tidal currents, while intercalated conglom erate beds in the higher parts of the suc References: TiwARI & Rov (1973); TRbGER & cession reflect high energy events with ULBRICH 1971) TROGER 1967); VOIGT 1929). ( ; ( ( scouring and rapid deposition. These con- 23
2.2 Teufelsbachtal section near boundary). The Middle Triassic beds are Blankenburg (Fig. 17) overturned. Both the Blankenburg Forma (by K.-A. Troger & F. Horna) tion and the Middle Triassic sediments are deformed by post-Early Campanian move Location and grid reference: TK 25, ments. 4131 Derenburg, R: 4425450, H: 5742730. The outcrop is situated 3 km northwest of Palaeogeography: The shoreline of the Blankenburg adjacent to the road to Early Campanian sea was just in front of Heimburg (Fig. 2). the uplifted Harz block. During the Campanian, the flexure zone north of the Tectonic setting: Flexure zone north of Harz probably represented an archipelago the Harz block. An angular unconformity formed by island chains consisting of Lower between the Blankenburg Formation and Middle Triassic limestones. (lowermost Campanian) and the Hauptmuschelkalk (Middle Triassic) is ex Stratigraphy and lithology: The basal posed (Fig. 17). Type locality of the part of the Blankenburg Formation Wernigerode Phase (Subhercynian tectonic (?lowermost Campanian) is composed of movements at the Santonian/Campanian calcareous siltstones and fine-grained
Te ufelsbachtal Section; after Cloos, 1917 North - South cross-section through the flexure zone north of the Harz (without scale) SW NE
-- -- N
·.-\ '·-�.:> - ��f?!J.J. •·. !? Blankllnburg Forrnahon
0 2 3m L'===·=:.' --� Te ufelsbachtal Sedioni------.J Legend 3m Blankenburg Formation, - Early Campanian L::;] ? Heimburg Formation, �0 Late Santonian Heidelberg Sandstone 2 E:J Late Santonian Salzberg Mar1 CJ Middle Santonian Silt- and Sandstones 1---1 Triassic, Keuper 1 Limestones Triassic, Hauptmuschelkalk Er[2l Member (with borings) Anhydrite � Triassic, Anhydrite Member Limestones � Triassic, We llenkalk Member Conglomerate of reworked �; Triassic, Hauptmusehelkalk �; J Member
17. Lithostratigraphy of the Teufelsbachtal section. Fig. 24
sands tones. Fauna: The sediments of the Blankenburg The angular unconformity surface between Formation are not particularlyfo ssiliferous. the Blankenburg Formation and the Triassic The macrofauna mainly consists of frag basement is irregularly shaped and wavy. ments of oysters and belemnites. Complete This irregularity reflects differences in re belemnite guards ( Goniotheuthis) are very sistance to weathering of the alternating rare and are reworked. They belong to the hard limestones and softer marls compris phyletic lineage G. granulata-G. ing the Triassic (Hauptmuschelkalk) suc granulataquadra ta-G. quadra ta at the cession. Santonian/Campanian boundary. Because The Triassic limestones are intensively all of them are reworked, an Early bored. A conglomerate consisting of mid Campanian age is assumed. The microfauna dle Triassic limestones is found 1.2 m above is characterized by low abundance and di the unconformity. The pebbles are irregu versity. Benthic foraminifera belonging to lar in shape, poorly rounded and show the genera Psammosphaera, Marssonella, traces of boring. and Lenticulina have been recorded.
References: Cwos (1917). 25
2.3 Hoppenstedt quarry (Figs. 18, scribed in detail in Chapter 2.6 19) (Baddeckenstedt quarry, No. 6). (by F. Horna) Unit B (bedded limestone member): Location and grid reference: TK 25, Unit B shows significant higher carbonate 4029 Vienenburg, R: 4408000, H: 57633 50. contents than Unit A. It can be subdivided The abandoned quarry "Kalkwerk into 8 to 10 m thick cycles with increasing Nordharz" is situated 4 km west of carbonate content towards the top of each Osterwieck at the northern edge of the vil cycle. The microfacies is characterized by lage of Hoppenstedt (Figs. 2, 11). The calcisphere and foraminiferal mudstones quarry was worked until the early sixties and wackestones. The clay mineral compo of this century. sition changes from predominantly montmorillonitic in the lower part to Tectonic setting: Southern flank of the kaolinitic in the highest beds. A progres Fallstein salt structure. The NW-SE Fallstein sive shall owing of the depositional environ Anticline is 2 to 3 km wide and about 7.5 ment can be inferred. At the top of Unit B, km long. Its core is formed by Triassic there is an abrupt lithologic change (the sediments (Muschelkalk). The Upper Cre so-called "Fazieswechsel") from pure white taceous deposits dip at 30-40° SSW. coccolith limestones, traditionally termed "Arme rothomagense-Schichten", to red General remarks: The upper Cretaceous dish and brownish coloured marls and succession of Hoppenstedt (Cenomanian to marly limestones, collectively known as basal Coniacian) was subdivided by HoRNA Rotplaner at the base of the overlying Unit (1996) into four sedimentary units (Fig. C. This facies change reflects an hiatus that 19): is traceable throughout Europe (e.g. sub Unit A (limestone-marlstone-alternation), plenus erosion surface, the change from the • Unit B (bedded limestone member), Regensburg Greensand to the Eibrunn • Unit C (Rotplaner), Marls, and the Antifer 1 Hardground in • Unit D (thin-bedded marly limestone northern France). • member). Within the massive limestone beds, an up These units differ in their carbonate con to 0.05 m thick marl-seam (bed T-24, Fig. tent as well as in their microfacies and char 19) yields abundant fragments of small acter of sedimentation. pycnodonteine oysters, constituting the Pycnodonte Event. Owing to the lack of Unit A (limestone-marlstone-alterna stratigraphically relevant ammonites the tion): Because of the monotonous A-B base of the Upper Cenomanian is drawn rhythms of unit A, a continuous sedimen above the Pycnodonte Event horizon. tation with rhythmic changes of terrigenous The Amphidonte Event is marked by the input and/or planktic productivity is in occurrence of small exogyrine oyster frag ferred. These rhythms are interrupted by ments within a limestone bed otherwise coarser-grained beds rich in inoceramid devoid of macrofossils (bed T -1 7), 7 m debris and with typical post-event above the Pycn odonte Event. bioturbation (sensu SEILACHER 1982). Conse quently, they are considered to represent Unit C (RotpHi.ner): The basal part of event-beds deposited from suspensions. Unit C consists of reddish and brownish, The base of the Middle Cenomanian, cor bioturbated, flaser-bedded marls and marly responding to the Cunningtoniceras inerme limestones, and is distinguished by a sig Zone which is known from complete sec nificantly lower carbonate content (55 to tions in Lower Saxony (Wunstorf) and 65%) than Unit B as well as by lateral thick southern England (Lewes, Dover-Folke ness variations. Sharp contacts between the stone) is missing at Hoppenstedt. Besides marls and lateral variations of thickness biostratigraphic premises this is also sup indicate an episodic sedimentation (mud ported by well documented periods of flows) of the marl s (inoceramid resedimentation at the level of the prim us wackestones). The pelagic background Event. sediments (autochthonous calcisphere Unit A comprises the prim us Event and the foraminiferal wackestones and packstones), Mid-Cenomanian Event, which are de- represented in the overlying plenus Bed 26
(named after the belemnite Actinocamax plenus), are restricted to infilled burrows. The plenus Bed is a conspicuous, massive white limestone bed with a pink mottled upper part characterized by anastomosing stylolites. The carbonate content increases from 77 to 82% from the base to the top of the 0.6 m thick limestone bed. The microfacies of the plenus Bed is dominated by calcispheres, which comprise more than 50 % of the biogenic component. The mot tled and, in some cases, nodular appear ance of the upper part of the plenus Bed is caused by bioturbation. The numerous Th alassinoides burrows (omission-suite Th alassinoides) are filled with reddish sedi ment identical to the overlying marly lime stones during sedimentation of the so called Lower RotpUi.ner. 18. Sketch map of the Hoppenstedt quarry , Within the level of the My tiloides Event (see Fig. below), apart from inoceramid showing the two main marker beds. wackestones, inoceramid floatstones (rudstones) occur, which are interpreted to represent tempestites. Furthermore, in composition within Unit C is characterized creasing fragmentation of the inoceramid by the dominance of montmorillonite, as shells, caused by increasing erosion at the in the lower part of Unit B. The Upper base of the tempestites, indicates a shift of RotpUiner above the tuff TC, which usually the depositional area into a more proximal reaches a thickness of more than 1 0 m in environment. lnfilled Th alassinoides bur other localities, is completely absent from rows, described by WANLEss et al. ( 1988) as the Hoppenstedt section. tubular tempestites, show a depositional Unit C includes several events, providing environment dominated by storm events. distinctive stratigraphic markers: 1) the The succession above the Mytiloides Event Chondrites Event, 2) the Gastrochaena Ho is formed by several 0.2 to 0.8 m thick dis rizon, 3) the hattini Event, 4) the Mytiloides tinct limestone beds within the marls. These Event, 5) the White Boundary Bed (Wei�e limestones represent a more autochthonous Grenzbank), 6) the tuff horizon TC. pelagic sedimentation. The Chondrites Event, underlying the The coincidence of a mass occurrence of plenus Bed, is an horizon remarkably en Mytiloides hercyn icus and the first appear riched in Chondrites at two separate lev ance of Collignoniceras woollgari has been els. The Chondrites bioturbation of the reported at several localities in NW Ger upper level originated from the base of the many (ERNST et al. 1984; KAPLAN 1992). The plenus Bed, indicated by the paler and more hercyn icus Event therefore provides a good calcareous burrow infill. The facies change, marker horizon for the base of the Middle the Chondrites Event and the plenus Bed Turonian. The hercyn icus Event has so far provide excellent marker horizons within not been recorded from Hoppenstedt or this unit and facilitate correlation. from the Sohlde and Baddeckenstedt sec The Gastrochaena Horizon comprises a tions. Consequently, a hiatus around the flood occurrence of Gastrochaenolites in a Lower/Middle Turonian boundary can be marly, greenish coloured bed (T 5/6). inferred for these localities. Gastrochaenolites borings are inferred to The Middle RotpUi.ner, separated from the be connected with erosional boundaries Lower RotpUiner by a conspicuous lime (KRAWINKEL & SEYFRIED 1996) and are used as stone bed ( "Wei�e Grenzbank" or White an indicator of short-term bioerosion Boundary Bed), is characterized by increas (BRO E & AsGAARD 1993 ) . This horizon has ML Y ing carbonate contents between 83 to 90% so far not been reported from the correla and a microfacies that consists almost ex tive sections in Lower Saxony. clusively of calcispheres. The clay-mineral The hattini Event is marked by the sudden 27
m Biostratigraphy Lithology Eventstratigraphy Se -- ______�end 80l���!?.,l)� ? Grauweisse T 39/40 c Prionocyclus Wechselfolge limes�tone .!! german 02 c... 75 0 ""Micraster T 35136 marl marlstoneE2l � Subprionocyclus '"" Crel1rhynchia ' ' '. neptuni �' '�. ', .', ' event 1-- ::I , , marlB bed 70 ,,,,,,,,,,,,,,,,, 01 T 29 "" tuffTc � c intraclasts� 65 Ill ·;::... 0 Collignoniceras T25 hardgroundm woollgari 60 �Gl C4 shellm bed ,:0 T 23 "C j ""mari T, 1-- 0 55 T20 (PDB) "" 'M1ite Bounda Bed (Weisse Gren � ank) T 17 c I Ill 50 Mammites c... nodosoides 0 y�y�y�y�y�y�t,�y�y� ...... ,...... ,...... ,...... "" Mytiloides event �...... ,...... ,...._ C3 45 ) 0 0 0 0 0 T 13 ""violet marl ; Wa tinoceras 0 devonense ""hattini ..J event 40 nnnnn Neocardioceras T 5/6 "" Gastrochaeno/iles b. �/en us bed C2 jUddii & �Chondrites event f-- "" � 35 Metoicoceras facies change � c TO r=-.:. geslinianum B4 Ill j T -3 c f-- t Ill 30 E 0 83 Glc • (.J ... Calycoceras Amphidonte event 25 Gl • CL guerangen T -18 f-- CL ::I 82 20 Pycnodonte event - T -24 •
15 c Acanthoceras Gl (.J jul 19. Bio- and event stratigraphy of the Cenomanian, Turonian and basal Coniacian of the Hoppenstedt Fig. quarry. appearance of My tiloides hattini 3.5 m the plen us Bed (Fig. 19). Both the bottom above the top of the plen us Bed. A subdivi and top of the bed are strongly undulated sion into two separate hattini Events, as and show a stylolitic overprint. reported by ERNST & Wooo (1995) from An excellent inter-regional correlation is Baddeckenstedt, cannot be observed at provided by the tuff layer TC, 12.5 m Hoppenstedt. above the top of the White Boundary Bed Mytiloides mytiloides appears in abun (HoRNA 1995 ) . This tuff layer has been rec dance 7 m above the top of the plen us Bed. ognized in the Sohlde sections and also in This horizon is herein taken to mark the Westphalia (WRAY & Wooo 1995; WRAY et al. base of the widespread Lower Turonian 1995). Myriloides Event. The White Boundary Bed (Wei&e Unit D (thin-bedded marly limestone Grenzbank) is a conspicuous hard, splin member): Unit D begins with an incipient tery limestone bed 17.5 m above the top of hardground. These nodular, flaser bedded 28 limestones are rendered conspicuous by There is no ammonite evidence for the ex glauconitic pigmentation, yellowish colour, istence of the Hyphantoceras Event at and increased cementation. Their Hoppenstedt. The Cre tirhyn chia Event may microfacies pattern is characterized by represent the same stratigraphic interval, foraminiferal wackestones and packstones, since in condensed platform sections of calcispheres are less frequent. Glauconite southern England C. cuneiformis occurs and phosphatic bioclasts are present. The commonly in a hardground (Chalk Rock) costella tuslplana Event (ERNST et al. 1983) which yields the ammonite fauna of the which is taken to mark the base of the Up Hyphantoceras Event. per Turonian elsewhere in Germany, is ab The Micraster Event is characterized by the sent from Hoppenstedt because of a hiatus sudden appearance of advanced Micraster resulting from the hardground sedimenta (cortestudinarium group) above the mar! tion. Furthermore, the entire event succes seam T35/36 (Fig. 19). sion comprising fl int F , T , T , T , ME up 23 01 02 E to the Hyphantoceras Event is not repre o 13C values: In the basal pan of Unit C, sented at Hoppenstedt. An horizon (bed 34) the o 1 3C values rise continuously from 3.1 with abundant brachiopods ( Cretirhynchia to 4.99%c in the plen us Bed, reflecting the cuneiformis, Kingena elegans, Gibbithyris global Cenomanian/Turonian boundary subrotunda, and Orbirhyn chia cf. excursion (Fig. 19). The increase in values reedensis) occurs 5.5 m above the tuff layer agrees with published data relating to this Tc excursion in other areas (ScHOLLE & ARTHUR Above the nodular limestones thin, platy, 1980; HILBRECHT 1991; SCHONFELD et al. 1991; greyish-white limestone beds with interca UucNY et al. 1993). In the uppermost part lated diagenetic mar! seams appear. The of the plen us Bed, the values already start MicrasterEvent (see below) is the first Up to decrease, but the decrease of the values per Turonian marker horizon which has is more gradual than the previous increase. been identified within the Hoppenstedt In the Lower Rotplaner o 1 3C values decrease section. 3 m above the MicrasterMarl, there to 3.5%c. In the Middle Rotplaner the o 13( is a change to a rhythmically bedded marl values drop to 2.5 to 3%c and are here as limestone succession with a thickening up low as beneath the Cenomanian/Turonian vvard of the marls. This corresponds to the boundary excursion in Unit B. Grauwei�e Wechselfolge of Wooo et al. ( 1984), which can be seen in the Salzgitter Refe rences: BROMLEY & AsGAARD (1993 ); Salder section (No. 7). The carbonate con ERNST & WooD (1995); ERNST et al. (1983, tent fluctuates between 80 and 95% with a 1984); HILBRECHT ( 1991 ); HORNA ( 1995, 1996); decreasing trend up-section. KAPLAN (1992); KRAWINKEL & SEYFRIED (1996); ScHOLLE & Sc F LD Two events provide marker horizons within ARTHUR ( 1980); HON E et al. Unit 0: 1) the Cretirhynchia Event, 2) the (1991 ); SEILACHER (1982 ); Uuo,'Yet al. (1993 ); Micraster Event. WANLESS et al. (1988); WooD et al. (1984); WRAY & Wooo (1995); WRAY et al. (1995). 29 2. 4 Road-cuttings near Vienenburg provided their field data. (Figs. 20, 21) (by G. Ernst, U. Rehfeld & C. ]. Wood) Stratigraphy and facies: 58 m of Cenomanian beds were formerly accessible Location and grid reference: TK 25, on the west side of the Autobahn cutting. 40 29 Vienenburg, R: 360230, H: 575955 to The mar! facies of the basal Cenomanian is R: 360220, H: 57 5980. Road-cuttings of the exposed some 4 km away in the Wedde A 395 Bad Harzburg-Vienenburg Bach section on the southern flank of the Braunschweig and west side of the B4. anticline, and exhibits the normal fossiliferous character. The boundary to the Stratigraphy: The B4 section described Upper Albian is marked, as usual, by a comprises the hardground facies from the glauconitic marl horizon, which indicates Lower /Middle Turonian boundary to the the position of the sequence boundary and allochthonites of the Lower to ?basal Mid the transgressive systems tract of the sub dle Coniacian. A thrustmass of Cenomanian sequent Cenomanian transgression. age is intercalated within the Upper In the B4 road section, an olistolithic block Turonian. of Cenomanian material, previously decribed by ScHLOENBACH ( 1868) and ScHRbDER General remarks: The Autobahn cutting (1912) as the so-called "Cenoman-Keil" was made in 1972, before the event (Cenomanian wedge), is incorporated in the stratigraphical framework of the Upper Turonian succession. This consti Cenomanian-Coniacian interval was devel (ERNST & oo tutes a slipped mass W o 1995) oped. The section is now much degraded which became detached from the roof of in many parts and access is not normally the Vienenburg diapir in the course of the permitted. The historic section in the river upward movement of the Vienenburg cliff forming the eastern truncation of the halokinetic structure. The individual com Harli (ScHLOENBACH 1868; ScHRODER 1912), par ponents of this complex slide mass are de alleling the B4, seemed to be virtually for limited by marls, which acted as slide gotten. The two closely adjacent sections planes. As typically found with slide masses, provide an useful composite section from "Scheiterkalk" (limestone with a lath-like low in the Cenomanian to the middle pan structure) and phacoidal bodies are also of the Coniacian. associated. The fauna collected by T. In comparison to other exposures in the WAGNER-DouGLAS and ourselves indicates lower part of the Upper Cretaceous, the both Lower Cenomanian (Schloenbachia, Vienenburg section exhibits some special In oceramus virgatus) and Middle features. The Turonian here is represented Cenomanian (Acanthoceras rhotomagense) by a very much reduced succession, which components. The Middle Cenomanian fos is consequently, particularly in the lower sils include elements from the primus fauna and middle part, characterized by (Hemiaster griepenkerli) as well as from the hardgrounds and the development of the time range of the Mid-Cenomanian Event so-called Conulus facies. A thick series of (Holaster subglobosus) and the vicinity of allochthonous sediments is intercalated the Pycnodonte Event. into the higher Lower Coniacian autoch The "Cenoman-Keil" was formerly consid thonous succession, providing evidence of ered to be restricted in its lateral extent to one of the main (llsede) phases of the B4 section, with only incipient indica Subhercynian tectonic activities. Another tions of disturbed sediments in the adja noteworthy feature is a large olistolith of cent Autobahn section. However, the recent Cenomanian sediments situated within and discovery of a large limestone phacoid with interrupting the Turonian succession. This Acanthoceras cf. jukesbrownei and is interpreted as a slide mass, which prob In oceramus cf. atlanticus, situated either ably became detached towards the end of within or underlain by debrites on the west the Early Coniacian. All the strata are over side of the Autobahn cutting, indicates that turned. the Cenomanian olistolith may have for The Upper Cretaceous of the Vienenburg merly extended much farther to the west, An ticline is currently the subject of inves perhaps even beyond the cutting into the tigations by I. MAUSA, T. WAGNER-DouGLAs and area of the Harliberg itself. F. WIESE (Berlin working group), who kindly The Cenomanian/Turonian boundary sue- 30 • !5 eventsand remar1111 micro- zor.e 11thology fossils 0 ifacies J t----.c===---+------+------�_ 0 1--large------+ phacoids .f.:....r-- w:,.:....i ...__: ---II---Myf-SQJ....:'101de�· , • "- ,-f. � -�._-. Cenoman1an � n_ , brittled limestones , � l'9 ·� · wedge "Schelterkalke'' I 37 3S ...... 1 Echmocorys sp Mytl/oide$ c 33 ...... ,! IBb•atoldiformis ...... !!c .... .1 E :;, ...... l1 t- � " 29 :: .. :::::·::· ·1 . . -�" . � :stria==�rlCU$ . . " 27 �� " - - -�-�� 2S " . / CUVIerilmorphotypes ,, large �'----· 0 )- Conulus raoes .!!c c·�/noceremus 17 J:=:::::;;;�$: " E lamen:Ju � GJ lnocerwmus 15 � cuvrerii -�· lnoceramus "�--=��� i .. . " ap�eal•s debris I " now �-��j ,, 0 C. subrolundus 1-g;- "Green HG" " • n ' I Jamarclu •• • � hiatus l.epiaNs - :� � Conulus l.aJWeni " ...... 0•O subrotundus � hardground = - - • ./ Whileyellow Boundary Bed" ? .. • Myfiloldes Orbimynctr•e 'I> _j � a-- :� :�. myflkNcMS 7 �i .,.,.,l/� ���" I Cenomanlan wedge event atlantraJs � Pycnoc:lonte ? � I � '"•-----� " . I V Acanlhoceras Cyrnaroceras i .!! l.allaniiCUS sp kasbrownei ,_ -< l; �ij __ • Acanlhoceras � 1 I � E0 i Acanthoceras � motomagensa :o __:!.� Tumlrtes .2 e :::::.- ; molorn8gensa � sctrauchzenanus � r-V ------Euthym•pecten '?' O Msnren.aras •_ beaven Schloenbachlal\ri'f1&fus •-•-•- i � d1Mon1 m j Schloenbactr•a even! ..J �- sp. ;;. Fig. 2 0. Turonian section of the road cut, Vienenburg structure (after 1996) B4 WAGNER·DouGLAs cession was documented in detail on the marked hiatus by deep red, then followed east side of the Autobahn cutting (HILBRECHT by variegated marls. These marls are of 1988; HILBRECHT & DAHI\IER 1994). lt is char tempestitic origin exhibiting a bioclastic acterized by an extremely condensed suc matrix mainly composed of inoceramid cession developed in Rotplaner facies. The fragments, gutter casts and, slightly higher pre-plenus sequence and the plen us Bed up-section, grade into lenticular together total only 0.5 m, but nevertheless tempestites. Rising energy levels are docu exhibit the characteristic Ch ondrites Event mented by an increase in the size of the and the tripartite subdivision of the plen us channels and in the number of intra- and Bed. The plen us Bed is overlain with a extraclasts. This facies is typical of a car- 31 bonate ramp. The first Mytiloides Event is overlain by a marly debrite. The marly found only 0.5 m above the plenus Bed: limestones are succeeded by the nodular the morphotypes here are closer to M. and splintery so-called Con ulus facies, Jabiatus than to the more common M. which was described, among other work mytiJoides, a fact which HILBRECHT & DAHMER ers, by ScHRbDER ( 1912) from the east side ( 1994) attributed to possible ecomorphic of the Vienenburg structure.Apart from the factors. It is noteworthy that the tempestite typical echinoids (C. subrotundus, facies has a greater vertical extent than in Sternotaxis plana, Ech inocorys gra vesi), the the nearby comparative sections. Both the fauna comprises mainly Orbirhynchia and early establishment of carbonate ramp sedi other brachiopods. According to the mentation and the small thickness of sedi inoceramid biostratigraphy, the Con ulus ment indicate a significantly shallower fauna may well be situated close to the bathymetric position than in the case of Middle/Upper Turonian boundary, in that other Rotplaner sections. Middle Turonian index taxa ( Inoceram us The stratigraphic condensation character lamarcki and related forms) are associated ized by hardgrounds and the Con ulus facies with rare Upper Turonian elements. continued into the early Late Turonian (Fig. In the Upper Turonian, above the Con ulus 20). In the B4 road section, the succession facies, the sedimentation pattern "normal begins with the Cenomanian/Turonian izes" to some extent. Marly limestones with boundary interval. At the base of the sec sporadic marls are typical. It has not yet tion, Lower Turonian red marls with been possible to correlate the marl seams My tiloides are exposed. These are overlain of the B4 section with those logged by by a complex tripartite unit of hard beds, SEIBERTZ (1972, unpublished) in the Auto about 3 m thick, which form a conspicu bahn section. It remains unclear whether ous projecting ridge. This unit is composed or not the event bundle in the vicinity of of hard, white, pink and ochre-coloured Marl ME or the Hyphantoceras Events are limestones within which there are several developed in these sections. A similar situ hardgrounds, as well as marl seams and ation may be found in the Hoppenstedt mar! partings. It is not known whether or section on the Fallstein east of the not any of these marls are of vulcanogenic Vienenburg structure, where these events (tuff) character, rather than merely detri are represented by a non-sequence (HoRNA tal marls. Analyses for rare earthelements 1995 ). In the Beuchte quarry, situated on by D.S. WRAY (University of Greenwich) in the northern margin of the Vienenburg dicate a detrital origin. It is likewise unclear structure, some 4 km WNW of the B4 sec where the White Boundary Bed with its tion, the Upper Turonian is largely reduced overlying M0 marl is situated within this in thickness, but here both the ME event complex. From the very limited inoceramid bundle and the Didym otis I Event can be ev idence, we assume that the entire unit recognized. However, the Hyphantoceras comprises a reduced equivalent of the Events have so far not been identified, al apicalislcuvieri Zone. The hardgrounds are though the underlying condensed penetrated by post-depositional brachiopod acme-occurrence, which nor glauconitized Th alassinoides burrows, and mally underlies these events, is well repre the surfaces exhibit irregularly developed sented. shallow grooves reminiscent of shrinkage Between the "Cenoman-Keil" and the or dessication cracks. allochthonous Middle Coniacian in the B4 The shallower water environment, indi section a some 15 m thick succession is cated by the hardgrounds, is further dem found, comprising an alternation of marls onstrated by the typical echinoid faunal and marly limestones with sporadic minor elements such as Con ulus subrotundus and allochthonite intercalations, including de a single Cardiaster truncatus. The facies and bris flows. On the basis of the inoceramid its associated fauna is closely comparable fauna, this part of the succession must be to that found at Wi.illenin Westphalia (ERNST long to the Grauwei&e Wechselfolge sensu et al. 1992). The hardground complex is Wooo et al. (1984). At the base of the sec overlain non-sequentially by pale marly tion the higher of the two Didym otis Events limestones with Inoceramus Jamarcki. Some is found, which approximates the additional hardgrounds are found in the Turonian/Coniacian boundary. Two beds, lower part of this interval, one of which is respectively 1.5 and 2 m above the base, 32 yielded typical Cremnoceramus of the event beds, that decreases in the middle waltersdorfensis and rotundatus-erectus part. Towards the top, the facies changes lineages, associated with Con ulus rapidly into coarse-grained event beds (Fig. subrotundus, Ech inocorys gra vesi, 21; phosphorite 10-12 ), which yield abun Sternotaxis sp. and Micraster ex gr. dant phosphorites pebbles as well as lime cortestudinarium. The occurrence of stone clasts and phosphatized sandstones. Con ulus is of particular palaeoecologic in Additionally, well rounded quartz grains up terest, since this genus is absent from cor to 7 mm in diameter occur. Overlying the relative sections elsewhere in Lower Saxony. allochthonous succession with a sharp con As this species is exclusively known to oc tact, glauconitic, decalcified and cur in context with shallower water envi crossbedded siltstones represent autoch ronment, reduced sedimentation, incipient thonous lowstand sediments that rapidly and true hardgrounds as well as rework grades transgressively into the Emscher ing, its occurrence here points to a continu Marls. ous shallow water environment and, to The fauna of these strata is poor. Only shark some degree, to condensation. The succes teeth, so far 16 different species, were sion ends with a sponge horizon, in which found in larger numbers (]. KRIWET, Berlin, numerous hexactinellid sponges are found pers comm.). Poorly preservedsponges are in a coarse inoceramid shell debris scattered throughout the section but may wackestone. Close above the sponge hori be enriched in distinct horizons that show zon, a bed with large fragments of characters of incipient hardgrounds. Sparse Cremnoceramus ex gr. crassus provides fragments of definite Cremnoceramus sp. evidence for the higher part of the Lower were found up to 1.5 m below the top of Coniacian. This bed yielded part of a guard the turbidites. Within the turbidites, of Pra eactinocamax-an extreme rarity at sponge-remains, remnants of a thin-shelled, this level throughout Germany-which on ostreid bivalve fauna as well as fragments stratigraphic grounds could well belong to of thick-shelled cremnoceramids can be P. paderbornensis. found. Important is the fragment of a Above the sponge horizon, the facies doubtful Volviceramus sp. from the upper changes rapidly into a succession of most phosphorite bed, which may indicate glauconitic calciturbidites. Intercalated are the base of the Middle Coniacian. approximately 13 very distinct beds that For the interpretation of the allochthonites, contain abundant phosphorite clasts. The it is particularly necessary to establish their turbidites are often stacked in thickening original age and provenance. Isotopic data, up/thinning-up cycles. In some cases, only provided by KREUZER (BGR Hannover) of the thickening-up or the thinning-up part glauconite grains in samples from the Auto was recorded. Thickly bedded, glauconitic bahn section give a range of ages from 88- calcarenites show a multiphase depositional 91 million years (ERNST et al. 1979), indi history with repeated phases of deposition cating that the glauconites were derived and erosion, indicating a long-lasting de from reworked Cenomanian sediments. The velopment and a persisting distributionary radiometric results were confirmed by fan system for this period. As thinning-up micropalaeontological analyses carried out or thickening-up, respectively, corresponds by KoCH (BGR Hannover), who found re to fi ning-up or coarsening-up develop worked Cenomanian foraminifera in some ments, each sequence can best be inter of the samples. This gives evidence that the preted as recording the sedimentation his allochthonites have also been derived from tory of one individual fan. A bed by bed significantly older formations. In addition, correlation from the old road cutting to the the presence of reworked Upper Autobahn is not possible. Therefore, the in Cenomanian and Turonian limestones is dividual beds are thought to be of only very documented by foraminifera within the limited extention. Each of these cycles is clasts, such as the Upper Cenomanian separated by a sedimentary unit that is Rotalipora cushmani and the Turonian rather dominated by either autochthonous Dicarinella hagni, Marginotruncana deposits or the Bouma D and E sequences pseudolinneiana and M. marginata. In of a turbidite. phosphorite beds 11 and 12, Aptian-Albian In its basal parts, the turbidite sequences sandstone clasts as well as phosphatized show comparatively high frequencies of pebbles of the Albian "Flammenmergel" 33 litho fossils lithology events and markerbed& units ;: :::>• ? " sp. - 0 " Cmmnoceramus 0 .c E "" - phosphonte 9 � i a. :::> c 0 50 ii :ll.. £ '5 "'0 .c:" e ="C c phosphorite - c:: 7 +8 0 ! ·- Ill � . ... � rl"' phosphorrte � ., •" E 40 6 u ;;; ., :::> 0 :>ou!!: " 0. " Ill ..0 • "' 0 "C"' .c " " phosphorite c:: :: •E 5 -u 0 g -o .. 0 ... = E .c:"' phosphorite - " � -� 0 " 0 " � .. '5 phosphonte .: 0" (shart< teeth3bed) 0!'! E" - ..E Ql 30 u £ !I: E " 0 "5 ...I 0"' "' phosphorite "' 2 c phosphonte "'0 0. 1 20 1st calciturtliditeglaucon1t1c '� -� - pebble bed �- llsede teclo-event he•actmelhd sponges ,.___ sponge beds (?) ex gr oetormts ___'-Ca. �-:::"' c scttloenbach, I ,. __ abundant debns of �- '" ' C att erectus large cremnoceram1ds _... , C rorundatus 0 C meonsrans _ thtckenmg up cycles 10 - :- C 'rassus 1 _ ,- , -.. (F c I _ .-::., �- ! ._ . 01 !! ••ltersDot1enSisC wanersdottetWS----. _ _ -- a - event - 1.1.1 �ymoiiS costatus -waltersdorf8nsrs11 event - � -�-- _-. 1 ' DldymotiS - ' Conc:mndhyrts sp --- .- · --- Glbbdhyns H�-?�?,_3! SP Fig. 21. Upper Turonian to Middle (?) Coniacian section of B4 road cutting, Vienenburg structure (after 1996). MAUSA were found together with one phosphatized known from the basal Cenomanian of the mould of Aucellina gryphaeoides, which is Floteberg section (Salzgitter Anticline) as presumably derived from the well as from the nearby Weddebach sec Flammenmergel (F. WIESE, Berlin, pers tion. However, diagnostic phosphatized comm.). The coarse quartz grains might remanie fossils have not been found so far. also originate from Neocomian sandstones. The abundant shark teeth associated with The abundant phosphorites could all have the phosphorites are in all probability pri their provenance in the Lower Cenomanian, mary fossils of Coniacian age. as is the case in the Zilly section (ESE of Comparing these lithologic data with those Osterwieck). Phosphorite clasts are also of the Cenomanian olistolith, it can be in- 34 ferred that during Cenomanian times, foredeep associated with a halokinetic glauconite- and phosphate-rich sediments structure, which contradicts KocKEL's inter were still restricted to the source area and pretation. Though the facies for the inter were only later reworked to produce the val from latest Cenomanian to Early early Coniacian allochthonites. The inter Coniacian in the Vienenburg succession pretation of these allochthonites is contro points to a shallow water depositional en versial. Our original interpretation (ERNST vironment of a swell, this area could equally et al. 1986) was that the Vienenburg struc well have been the rising Vienenburg ture itself functioned as the source area, halokinetic structure, rather than the and that the allochthonites moved from the Fallstein block. roof of the diapir in the course of the Ilsede The old clay pit adjoining the northern end Subhercynian tectonic phase. In our view, of the B4 section is used as a waste disposal this hypothesis is supported by the fact that site today, but it probably exposed auto the allochthonites were obviously restricted chthonous Middle Coniacian in Emscher to the eastern flank of the Vienenburg Marl facies. This interpretation is supported structure. In contrast, KocKEL (in BRONING et by the record of an involute inoceramid al. 1987: Fig. 29) has reinterpreted the en (ScHRODER 1912), probably a Volviceramus. tire Vienenburg "Anticline" as represent A few hundred metres NNE of this ing a pile of Mesozoic sediments that had Coniacian clay pit, dark marls with a sparse slid south west from the roof of the rising marofauna were temporarily exposed in the Fallstein basement block and had come to floor of the Oker valley between the B4 and rest in its present position, where it became the railway. The index fossils Gonioceuthis subsequently modified and uplifted by salt westfalicagranulaca, G. granulaca and injection. KocKEL argued that typical fea Actinocamax verus prove a Mid- and Late tures of a halokinetic structure, such as pri Santonian age for these sediments. mary and secondary marginal troughs ("Randsenken"). are not developed in the References: BRONING et al. ( 1987); ERNST & Vienenburg "Anticline". In his view, this Wooo ERNST (1995 ) ; et al. (1979, 1986, and other gravitational slide structures are 1992); HILBRECHT & DAHMER ( 1994); HILBRECHT of Santonian age. However, the existence (19 88); HORNA (1995); MAUSA (19 96); of Lower Coniacian allochthonites in the B4 SCHLOENBACH (1868); SCHRODER (1912); SEIBERTZ section presupposes the existence of a (1972, unpublished); WAGNER-00UGLAS (1996); Wooo et al. (1984). 35 2.5 Glockenberg section (Figs. 22-26) of the Salzgitter-Goslar area was highly vari (by ]. Mutterlose) able during the Valanginian-Aptian inter val. The Harz massif, less than 10 km to Location and grid reference: TK 25, the south, was probably not covered by sea 402 8 Goslar, R: 3598500, H: 5761237. The in Early Cretaceous times. From here, elon abandoned mine "Georg-Friedrich" is situ gated SW-NE striking swells extended up to ated about 10 km northeast of Goslar, about 15 km into the NW German basin to the 2 km east of Dornten (Fig. 22). The shaft north. The deposition of the iron ores of was operated until 1968 and subsequently Salzgitter was controlled by these penin fi lled in. The disused iron ore pit sulas, causing abrupt lithologic changes in "Glockenberg" is situated about 100 m a shallow marine nearshore environment. north of the mine. Up to 100 m of iron ores accumulated in synsedimentary Y -shaped graben struc · Tectonic setting: Western flank of the tures, aligned parallel to the strike of the Salzgitter Anticline. The NW-SE striking salt Strata (KOLBE 1962, 1970). structure is 2 to 3 km wide and about 20 km long (Fig. 22). The axis of the salt-in Facies and Stratigraphy: The north face duced anticline, which is here about 200 of the pit exposes in its easternmost part m farther east, is marked by Triassic dark bituminous shales (Lower Toarcian, sediments (Buntsandstein). Early Creta Posidonienschiefer; Fig. 24). The ceous iron ores rest with an angular Posidonienschiefer, which yields unconformity of up to zoo on Toarcian lnoceramus dubius, was deposited under shales and Aalenian clays, indicating pre anoxic conditions and reflects a widespread Cretaceous movements. oceanic anoxic event (OAE). More than 5 m of black clays and marls of late Toarcian Palaeogeography: Eastern part of the NW and Aalenian age follow above the German Basin, a few kilometres north off Posidonienschiefer (Dorntener Schichten). the fo rmer coast-line. The palaeogeography About 7 m of coarse clastic ironstones of Early Cretaceous age rest with an angular unconformity on the Aalenian clays (Figs. 23, 24). The iron ores consist of reworked limonitic fragments of formerly sideritic B A nodules. The surfaces of the fragments are smooth and have been polished due to re working in a nearshore shallow marine en vironment. Reworked ammonite fragments Fort una indicate that the coarse clastic fragments �"- Neocomian lronore originated from Early and early Mid ,,,_�nterrupted by the jurassic sediments exposed nearby. Frag •.·, Lower Albian ments of Triassic origin are extremely rare. Tranagreaaion Iron ooids are less common, but occur in \ the lower part of thesection (beds 99, 100). 8? The iron content in the Glockenberg sec / tion reaches up to 40%. The clastic iron stone is embedded in a fine-grained clay mar! matrix. Intercalated are several lime Eisenkuhle stone beds varying from 0.6 m to 0.2 m in thickness. These horizons are less rich in limonitic clasts than the clays and marls. Further to the west the iron ore is overlain I km 0 2 -'.A by glauconitic, sandy clays of Early Albian age. This 40 m thick succession correlates with the Hilssandstein, which was formerly exposed in the Morgenstern section about 2 2. Geologic sketch map of the southern part of Fig. 2 km further southeast. Strata of mid the Salzgitter anticline, showing the outcrop of early Cretaceous sediments and locations of former ore Albian age consist of 10 to 15 m of clay, mines. yielding the belemnite Neohibolites 36 to all of the ironstone succession in GlockenbergI N-Fece Glockenberg. These stratigraphic interpre tations are based on the following obser vations: Oolitic iron ores are common in the Upper Hauterivian, they are, however, absent in the Barremian. Since most of the iron ores south of Liebenburg are clastic in their origin, KoLBE et al. (1984) inferred a Barremian age for the ore deposits in the southern part. Due to the high carbonate content a Hauterivian age is tentatively assigned to Legend so m the lowermost part of the Glockenberg sec tion, which directly overlies the Aalenian 0- clay. RODIGER (1932: 291) mentions two ... ---· e Glockenberg 0 1: .._ 0 .!! � c::: CL :::J -:: "D E ..5! Lithology - Ill 11 0 :::i! ID(J)O 2 3. Sketch of the north face of the Glockenberg Fig. section (modified after KoLBE et al. 1984) _ minimus (minimus Clay). The Late Albian I'll is represented by 80 m of siliceous marls ( Flammenmergel). > Stratigraphy of the iron ores: The exact age assignment of the Early Creta ceous ironstone formations in the Salzgitter .. area is still debatable. Due to differences in lithology and age it is possible to differ entiate between a northern and a southern I'll area of sedimentation. The village of Liebenburg marks the boundary. In the northern area, ammonites and belemnites provided a solid biostratigraphic frame work for dating the different iron ore - lenses. Belemnites, in particular, have = proved to be extremely useful (Figs. 25, 26). :--�02. -00�0--0� -_ _ _ � _ Iron ore sedimentation in the Salzgitter area - - _ _ _ _ - - .. _-_-_ _ 92 possibly started in the Late Valanginian, the rn - Late Hauterivian is characterized by oolitic �. ------m - ores, which are present only in the north. - -- = The main ore accumulation occurred in the -- - -= == - Barremian, when conglomeratic ores were - deposited. The Aptian is characterized by sandy and partly oolitic iron ores. 1: 11 85 KoLBE ( 1962) suggested an Hauterivian age .�. ,,, u .._ for the basal partof the succession exposed '- ···· 11 0 - in Glockenberg. This part is enriched in car 1- t bonate. Most of the 60 m section comprises - t- sediments of Barremian age. More recently 2 4. Stratigraphy and lithology of the Fig. KoLBE et al. ( 1984) assigned a Barremian age GlockenbergI section. 37 u ·� V: STAGES Ammonite zones 0 Belemnite zones c:: 0 NW c. Europe ....0 u - "'0 Srmbirskites discofalcatus (C.) t'7- Simbirskites gouschei "":) e.tltr, (C.! o:::::0-�-.::� z � 1- ·1, . ;11 V. t.J < L � c < Simbirskites (M. ) staffi :s,.-. � - ..l <= :-.:rM·b·-·;r � :.J-- .... a:l .C�-gu - Aegocrioceras Hibolites jaculoides v.:: =: spp. i � r-- 1- Endemoceras regale .... � CJ Cll) < � :: - - Endemoceras noricum ..l - ; V: :5 CJN < Cll) ' � Endemoceras amblygonium ·""'�-.,., • • .. b (; < . • ::.:: Elemceras paucinodum Acroteuthis.. acmonoides ' Drcostella tuberculara t---- ProdichoromDides ivano,·i Dichoromires bidichotomoides Dichoromires triprvchoides z i: < Dichotomites erassus - � z Prodichotomites poh·tomus - Acroreuthis acrei .. Prodichotomites hollwedensis - Polyprvchites sp haeroidalis z c::: < Polypr.·chites clarkei ::":' :�=� ..; Polvprvch11es multicosrarus < � Polyprvchites pavlowi • .... ; • I ."". t' < Plarylenuceras rnvolutum :·" � '" Plar."ienticeras heteropleurum �,;� QAcroteuthis kemperi Plar.•lenriceras robusrum J Peregrinoceras albidum Surites srenomphalus '• ·,· · .. . · . � Surites icenii .. .. I z -<; . Hetoroceras kochir . < � ... :.:J - Acroteuthis explanroides rr. Runctonia runctoni < - = Subcraspedites lamplughi =: :.; = ::; Subcraspedites preplicomphalus I er:: Subcraspedites sowerbvi < � Subcraspedites primtivus �Acroteuthis lateralis Fig. 2 5. Bio- and lithostratigraphy of the Berriasian-Hauterivian interval, showing belemnite species most significant for biostratigraphy. Simbirskires from the lowermost part ofthe closed down and abandoned. section, supporting a Late Hauterivian age. The iron ores are preserved in lenticular Future finds of belemnites might provide a bodies of 1 to 2 km length and up to 100 m definite age assignment. thickness. The lenses are aligned along the western and eastern shoulder of the Genesis of the iron ores: The Early Cre Salzgitter Anticline over a distance of 20 taceous iron ores of the Salzgitter area have km. The sedimentation of the iron ores was been economically important from about controlled by epeirogenic factors, in par 1940 to 1960, when they were mined ex ticular by a highly variable tensively. Today all mines and pits are palaeogeography. The ores were deposited 38 STAGES Ammonite zones 6 � Belemnite zones £ ·u NW-Europe ·- "' ..J'- Stoliczkaia dispar ' � Neohibolites praeultimus <:· 3 I = - E '-l <>u� !- Mononiceras inflatum < Neohibolites o;r;ycaudatus � �� ..;: · ...:: == Dipoloceras cristatum -s;;:... -� u... s z Euhoplites lautus "' < �"2 � a:l- - Q Euhoplites loricatus .o = = Neohibolites minimus "".::: f""': ..;: ' . - Hoplites dentarus c:.:. .:§5I .§ C: < ::!: -!'J Douvilleiceras -� - mammillaJum � -66'2 Leymeriella regularis Neohibolites minor c:-.= " ii <: � I :r.c--\0 < Leymeriella tardefurcaia '-l Neohibolites Proleymer�el/a schrammem strombecki '• <::.::1. : i :: i Hypacanthoplites jacobi Neohibolites )9 ... . :j Acanthoplites no/ani wollemanni "' < : : <) � � '"' � t;;; c:oo �-::- .... Parahoplites nutfteldiensis Neohibolites inflexus = .c:: = ' ·· . � j ' l · . 1 � 2 � <::::.::: :.r. ·- -.cI --:; �- Ep icheloniceras tschernnchewi Neohibolites clava � z ' . .. :::::::1 < < -- ��_:. - Tropaeum drewi , - -::::; !- ...... •' :. Tropaeum bowerbanki <:: � . . ; 1 ' I . I .. < :::::i Neohibolites ewaldi ::; Deshavesites deshawsi <;I') Cll: ;.., < t;;; � 0 c:oo � Prodeshavesites tenuicostatus .. ..J=- O.n-teuthis �� ..,_ Paraneyloceras bidentatum ::1 VI depress a �;,�::-,,.;:; ...... ··;·] 0 SimanC\·Ioceras srollevi - Orvreuthrs !:!: or. Ancvloceras e m germanica .....:;:::::: :.,; inn xu -· .. . � z ,- : 1 - Parancvloceras denckmanni - < O.nreuthis � - ParanC\'loceras e/egam . - -""' brunsvicensis . · (· ·:::: · ·7 . I . . ... , . ..,. ;.;: = : ) -::::; = Hoplocrioceras fiss1cosrarum · j < :SE:.�� in synsedimentary Y-shaped grabens and Aptian. Aptian ores or Albian sediments halfgrabens. The greatest thicknesses of ore cover the ore lenses. The strike of the iron deposits can be observed next to the fault. ore lenses corresponds to the axis of the Ore deposition and subsidence of the Salzgitter Anticline, subsequent movements graben occurred simultaneously. First, caused the steep inclination of the ore oolitic ores were deposited in the Late lenses. Hauterivian, while subsequently thick clas tic ores accumulated in the Barremian and References: KoLBE ( 1962, 1970); KoLBE et al. (1984); RODIGER (1932). 39 2.6 Baddeckenstedt quarry (Figs. 27- Marl-Limestone Rhythmites: This unit 2 9) (ea. 20 m) comprises alternations of thin (by C. j. Wood, G. Ernst & U.Rehfeld) ner, marl-rich beds and thicker marly lime stones up to and including Mm and the over Location and grid reference: TK 25, lying limestone. The marls typically have a 3927 Ringelheim, R: 3584000, H: 5774000. sharp basal contact and grade up into the The abandoned limestone quarry lies NW overlying limestones. The sediment is com of Baddeckenstedt east of the B6 between posed of calcispheres, foraminifera, Hildesheim and Goslar. coccoliths, inoceramid prisms and, at some horizons, a significant amount of sponge Stratigraphy: Lower Cenomanian lime spicules. The marl-limestone couplets vary stone-mar! rhythmite facies to the "Wei�e in thickness and degree of lithification. The Grenzbank" between the Lower and Mid sequence of couplets can be matched in dle Turonian RotpHiner. detail with the cyclostratigraphy of the cor relative succession in the Anglo-Paris Ba Tectonic setting: The quarry is cut into sin. There, the rhythmicity is interpreted the side of the Rasterberg on the S flank of to be orbitally controlled, corresponding the Lichtenberg Hohenzug at the point to the 20 ka cycle (precession) of the where it curves round tojoin the Hainberg Milankovitch band (GALE 1995). Stable iso structure in the tectonically disturbed NW tope evidence shows that the limestones corner of the Ringelheim (or Innerste) represent warmer sea water temperatures Syncline. The position of the quarry at the than the marls, with a maximum difference intersection of two major structures is ex of 4"((E RNST et al. 1979; DITCHFIELD& MARSHALL pressed in complex tectonics with several 1989). Bundles of five couplets terminat fa ult systems (BADAYE 1986). Of particular ing in a more strongly developed limestone, importance are the stepped tension faults, indicating the effect of the eccentricity cy typically throwing down SE towards the cle (100 ka), cannot be recognized at centre of the syncline. The displacements Baddeckenstedt. The underlying on these faults can reach ea. 6 m. The com argillaceous Cenomanian marl and the plex tectonics probably resulted from in Albian/Cenomanian boundary succession version of the Lichtenberg Hohenzug dur are not exposed in Baddeckenstedt, but the ing the Subhercynian Ilsede Phase. The basal Cenomanian transgression surface faults are inferred to have developed as may lie some 10 metres below the floor of sediment masses slid gravitationally from the quarry. the rising and tilting massif into the basin The Marl-Limestone Rhythmites contain to the south (BRONING et al. 1987). two distinctive event-bundles, which are described in detail below: 1) Sponge Beds Lithology and lithostratigraphy: The and Mariella Event, 2) "The Rib", ea. 70 m succession can be subdivided into In oceramus virga tus acme, Orbirhynchia the following three formations: Event, and "The Double Limestone". Cenomanian Marl-Limestone Rhythmites Near the base of the Baddeckenstedt sec • and Transitional Beds (almost 20 m): tion, the lowermost parts of a some 20 m Lower Cenomanian to lowest Middle thick rhythmically bedded marl-limestone Cenomanian. This unit is divided into a succession are distinguished by at least two lower, rhythmically bedded succession, conspicuously lithified coarse arenitic lime and a higher, less conspicuously, or even stone beds rich in inoceramid and echinoid non-rhythmic succession (Transitional debris which alternate with marlier lime Beds), which includes several, some 0.25 stones and marls, respectively. These lime m-thick, dark marls (M11-M1J in ascend stone beds are often enriched in the anas ing order. For descriptive purposes, these tomosing lychniscosan sponge Becksia, two successions are treated separately. which lead to their designation as "Sponge Cenomanian Limestones (ea. 22 m): Beds". The upper, main Sponge Bed also • higher Middle Cenomanian to lower Up yields poorly preserved moulds of ammo per Cenomanian. nites including Schloenbachia, Rotplaner (ea. 23 m): uppermost Upper Mantelliceras, Austiniceras, and Mariella. • Cenomanian to Middle Turonian. This is believed to be the level at which several Neohibolites ultimus were found 40 sub sequence m litho- and event slraligraphy hiat• and condensat•on slratlgraphy or M Teuto 0 h1atus f-=-=-o---=_. wllote• T boundary bed th1ckemng up seQuence With M. hercymcus + hiatus Concmndhyns Mytlioides hattint event hattrm M. 11 M. hattmr event I calcilurbidlles JUddli lish shale N. pienus bed with basal Chondntes event c: <11 lacoes boundary "E 40 E<11 0 c: coccolith (.)Ill gueranger1 limestones Q; Q. Amohu:Jonle event Q. ::> rholomagense(= Arme Sch1chten) - 30 A fukes Pycnodonle limestone browner Pycnodonte eve�t c: <11 sllant,cus event E r E., rhoromag. 0 c: + r acurus nodular beds Ill (.) Mld-Cenomanian event Ill 20 i5 "'0 rhotomag. � + r costatus onmus event urr scneuchu:nanus MlTl Orbirhynch1a event "'c: "E"' M_ au:om E 10 v11gatus acme 0 c: (.)Ill iD Hypotumllles 5 � Marmlla event sponge bed sea le el M saxb1i v + Fig. 2 7. Lower Cenomanian to Middle Turonian lithology and stratigraphy of the Baddeckenstedt quarry . inside cemented sponges. The thicknesses bivalves tend to form the base of both of both beds are not constant in the quarry marker beds. These beds were mentioned but swell and thin laterally between 0.2 and from the Hoppenstedt area as well (HoRNA 0.4 m. They are marked by sharp contacts 1996). against the subjacent marly layers; their Biostratigraphically, the arenitic beds be transition into the superjacent marl layer, long to the base of the dixoni ammonite instead, is more gradual. Gradation can Zone, which follow the argillaceous Lower often be recognized. Densely clustered, of Cenomanian marls of the subjacent ten double-valved large inoceramid mantelli ammonite Zone. 41 2 8. Sketch, drawn from photographs, of the NE corner of the Baddeckenstedt quarry, showing the most Fig. important Cenomanian events. The limestones comprise inoceramid It may well equate with the horizon of large, echinoid packstones to grainstones with a poorly preserved, glauconitized turrilitids patchily well winnowed mud fraction. in the Second Inoceram us Bed in eastern The bioclasts of the matrix average 1 mm. England (the so-called "Turrilitid Plane" of They are rounded and almost completely jEANS 1968). micritized. Many of the echinoid fragments "The Rib" is a conspicuous, 0.2 m thick exhibit syntaxial rim cements. limestone situated some 6 m below M111 and The packstones and grainstone microfacies tending to weather proud. It is a key ele of the arenitic limestone beds indicate shal ment of the Cenomanian cyclostratigraphy lower, more agitated water environments. (the limestone of couplet B11 of GALE 1995: Micritization of the bioclasts and homoaxial Fig. 4), and can be traced from England as rim cements around echinoderm fragments far as Hoppenstedt. At Baddeckenstedt it even hint at vadose diagenesis. Shallow yields well preserved Mantelliceras dixoni water conditions are likewise supported by and Inoceramus virga tus. The immediately the occurrences of charophyte gyrogonites overlying couplets are particularly rich in and dasycladacean fragments (ERNST & ammonites, notably Schloenbachia and REHFELD in press). The sharp contacts against Mariella, associated with In oceramus the sub- and superjacent marly calcisphere crippsi. This constitutes the Schloenbachial foraminifera wackestone, the sudden facies crippsi Event of BADAYE ( 1986 ). change and the gradation suggest an In bed 121 of BADAYE ( 1986) and in the un allochthonous origin with a probably derlying marl bed 122, there is an acme tempestite character from a shallower wa occurrenceof bivalved Inoceramus virga tus ter source. associated with common Schloenbachia, The large inoceramid valves at the base of In oceramus crippsi and Mantelliceras these beds are autochthonous, being inter dixoni. This corresponds to the virga tus preted to form some kind of "Obrution acme in the likewise carbonate-rich cou Lagerstatte" (see BRETT & SEILACHER 1991). plets above "The Rib" in southern England. The fast entombment by the tempestitic Orbirhynchia mantelliana ranges over some sediment favoured their good, even dou 2 to 3 m, with an acme occurrence in lime ble-valved preservation. stone-bed 119 of BADAYE (1986). A well-marked acme-occurrence of com Acompsoceras, Forbesiceras and monly large turrilitid ammonites associated Austiniceras are also recorded. This with Inoceramus crippsi, found in a marl Orbirhynchia Event corresponds to the low about 1 m above the Sponge Beds comprise est of the three Orbirhynchia Beds in the the Mariella Event. Omission is indicated Anglo-Paris Basin. by erosion of the upper surfaces of the The massive, prominent "Double Lime ammonites. The event is also found at stone" (although here only inconspicuously Hoppenstedt and it can apparently be bipartite) with its underlying Orbirhynchia traced to Westphalia (KAPLAN & BEsT 1985). Event is another key element of the 42 Cenomanian cyclostratigraphy and consti the Cenomanian Limestones. As noted tutes a combination of couplets B23 and above, there is a major hiatus and inferred B24. The top of this limestone at sequence boundary at the base of these Baddeckenstedt is extensively burrowed by beds. At this level ( 1.25 m above M11) there Th alassinoides, and GALE ( 1995) reported is a some 0.4 m thick horizon exhibiting at that there was a significant hiatus at this least three calciturbidites (ERNST & REHFELD level, involving ea. 27 m of the highest in press). BARTELS ( 1993) reported a signifi dixoni Zone succession developed at cant increase in grain size of the sediment Wunstorf, west of Hannover. The bed is very ea. 1 m above Mw He also recorded an in fossiliferous, yielding many ammonites in crease in the percentage of keeled plank cluding Schloenbachia, Austiniceras and tonic foraminifera in and above Mw Mini Acompsoceras renevieri. mum carbonate values were found in the The rhythmites are generally very highest marl (M,.). M,. is darker compared fossiliferous, quite apart from the previ with the other marls. It rests on a highly ously discussed event occurrences, and irregular surface and fills pockets and bur Plagiostoma globosum, Plica tula inflata and rows in the top of the underlying bed. Ap Euthymipecten beaveri are common in the proximately 1 m above M, there is an •. lower part of the section. Brachiopods in abruptchange to a unit of relatively coarse clude Mon ticlarella rectifrons and grained sediment, which includes the gas Grasirhyn chia grasiana. Most beds are ex trolith lens (see below). These sediments tensively bioturbated by Th alassinoides, rest with sharp basal contact on the under Planolites Ch ondrites. AR LS and B TE ( 1993) lying bed, and small pale brown to buff provided quantitative data for the phosphatic clasts are concentrated just foraminifera (including plankton/benthos above the base. Above M,a' the succession ratios), ostracods and bryozoa (see Fig. 29). becomes in general massively bedded and The rhythmites and the basal part of the arhythmic. Carbonate values increase to overlying succession were assigned to the wards the top, where rather coarse-grained Rotalipora appenninica planktonic limestones composed of inoceramid and foraminiferal zone. echinoid debris develop a marked The allochthonous coarse-grained arenitic nodularity at the level of the Mid Sponge Beds mark the "proximity" of a se Cenomanian Events. quence boundary, probably representing Three distinctive marker horizons can be lowstand sediments which were shed from recognized within the Transitional Beds: 1) a shallower swell area into the the Turrilites scheuchzerian us Event, 2) the Baddeckenstedt area. Since the subjacent Gastrolith horizon, 3) the Mid-Cenomanian beds are not exposed at Baddeckenstedt, Event. its distinct position cannot be defined. This The Turrilites scheuchzerianus Event is an sequence boundary probably equals the acme occurrence of large T. base of Sequence 2 of GALE ( 199 5) and of scheuchzerianus associated with Sequence 3 of RoBASZYNSKI et al. (in press). It Schloenbachia, Acompsoceras, Austi is unclear whether or not "The Rib" corre niceras, Euthymipecten beaveri, sponds to a maximum flooding surface at Grasirhynchia grasiana and inoceramids the top of the transgressive systems tract including In oceramus cf. reachensis, I. cf. of the sequence, with the overlying carbon schoendorfi and /. ? ex. gr. tenuis 0.3 m ate-rich couplets containing the virga tus above Mw T. scheuchzerianus is long-rang acme representing a highstand systems ing, first appearing in the higher part of tract. Evidence of a major hiatus at the top the Early Cenomanian dixoni ammonite of the burrowed limestone below M11 shows Zone, but the inoceramids appear to con this to be probably a sequence boundary stitute an early Mid-Cenomanian assem which, from its stratigraphic position, blage. ' would correspond to the base of GALE s About 1.5 m above M,. at least 350 (1995) Sequence 3. gastroliths associated with reptilian bones have been found in a lenticular occurrence The Transitional Beds: This unit com up to 1 m wide. The inferred provenance prises the succession from the second of of some of these pebbles from the region the four conspicuous marls (M11) up to the of the Harz points to a possible Mid Mid-Cenomanian Event and beginning of Cenomanian uplift phase preceding the 43 early Coniacian Ilsede Subhercynian inver the formation of the hardgrounds recorded sion phase (ERNST et al. 1996). The sur by tubular tempestites at Misburg (HPCF 11 rounding sediment contains En tolium quarry). The conspicuous shift in the ratio orbiculare and Ostrea incurva. The coarse of planktonic to benthonic foraminifera grained underlying sediment is similar to (second P/B break between M11 and M1b in that of the main primus horizon with BARTELS 1993) is inferred to occur on top of Actinocamax prim us as developed in Eng the nodular limestones. land. The macrofauna evidence from the The nodular arenitic limestones of the Mid scheuchzerianus Event points to an early Cenomanian Event at the top of the Tran Mid-Cenomanian date, although no un sitional Beds is characterized by the occur equivocally diagnostic Middle Cenomanian rence of Holaster subglobosus and large ammonites such as Cunningtoniceras or fragments of Acanthoceras rhotomagense Acanthoceras have so far been found. How with subordinate Aus tiniceras and ever, the identification by BARrElS( 1993: Fig. Turrilites costa tus (BADAYE 1986). Compared 8) of the key planktonic foraminiferal zonal to other localities, e.g. Wunstorf, where a index Rotalipora reicheli from midway be marked Austiniceras Event can be observed, tween M11 and M1• and above, suggests that Acanthoceras appear to predominate here the succession above the scheuchzerianus over Austiniceras. Apart from isolated re Event belongs to the narrow reicheli Zone. ports of Orbirhynchia, there is no evidence This zone is interpreted by German of the Orbirhynchia mantelliana occurrence micropalaeontologists as marking the base and the Sciponoceras baculoides acme that of the Middle Cenomanian, although else characterizes this event elsewhere. The where (e.g. Folkestone) it appears to mark nodularity of these coarse-grained lime the top of the dixoni Zone and may extend stones points to omission and incipient (English Channel, French sector) into the hardground formation (ERNST & REHFELD, in Middle Cenomanian. press). These beds are time-equivalent with The position of the prim us Event(s) remains fonu.1X pl••kL foramt/llt& lltd. pla&k1/bc'etll. bmlh. 1111111fncuon IDlii:ICd. ����orun.XIOllfvd. fnctiODbatlb. roram >l�pm...-IP: IN. fnc:tiaD ,,.. IOI'UI•• � ll!l-2� ..., ...... >1...... f'%): . ,.z...,.. => �· ,,. -i-- Ml · ['-, :::> t- < � 1-"rx � I== \1 11 ,_t- ,_1- t-� .. f=> """ 1/ --- r· :-- =" ....-!) Orbtrhl'ndun rvrnt t'- ,._ ,_1-" D. � 1:::::. C'\l!'nl · D � .. � Sr-lrlornhudlillll'if1:ulu.\ . I·• � � 1-- - .1=> "Th< Rob" 1 .. lf CK .... l=! � � �- 1-\.. lh � ;:> I .:: .., Spon�r Brd ntnl lr:\ p < -�� f �- ::;: �I-' '7'i:..:_t:=. F"" ::::- t:::. t ,. i ... :r·------• u • t • • . I • -- ... � tO .. I�• "' • 20 I for • plukL furuns bi"')....,..Oc sculphlrrdhalal nkJt0111 >l. problematic. On the planktonic several event beds of Inoceramus atlanticus, foraminiferal evidence these events should but only sparse occurrences of the epony lie above the scheuchzerianus Event. A mous inoceramid have so far been found specimen of A. prim us collected loose was at Baddeckenstedt. assigned on the basis of its matrix to bed In marked contrast to the relative abun 111, i.e. the bed between M and the nodu dance of the eponymous oysters in the a lar chalks (BADAYE 1986). It mustI be empha Pycnodonte Event, the Amphidonte Event sized that the critical succession is at comprises a relatively inconspicuous, present inaccessible. However, the succes sparse event occurrence in three closely sion which includes M1• and the bed with spaced marly beds, of small exogyrine oys the gastroliths is strongly reminiscent of ters (Amphidonte) and subordinate small the (dark) arlesiensis Bed and the pycnodonteine oysters. calcarenitic Cast Bed in the Anglo-Paris Apart from the event occurrences of oys Basin succession, i.e., the two main primus ters, these beds are almost barren of Event beds. The gastrolith Bed is also com macrofossils with the exception of parable with the Totternhoe Stone, which In oceramus pictus. By analogy with other is likewise an horizon in which reptilian areas, the interval is placed in the bones are found. Calycoceras guerangeri Zone, but no am A sequence boundary can be placed at the monites have been found at hiatus between the top of the "Double Lime Baddeckensted t. stone" and the overlying M11• In the absence The relatively coarse-grained bioclastic of definite evidence for the main prim us sediments of the Pycn odonte Events are Event, the flooding surface and the trans interpreted as a condensed transgressive gressive systems tract cannot be identified lag superimposed on a sequence boundary. at present. In analogy with interpretations This is variously taken to mark the base of of correlative sections elsewhere (OwEN the fourth (GALE 1995), or the fifth (0WEN 1996), the Mid-Cenomanian Events may 1996; ROBASZYNSKI et al., in press) correspond to a maximum flooding surface. Cenomanian sequence. The maximum flooding surface is considered to lie a short Cenomanian limestones: Above the distance above the massive limestone. OwEr-.: Mid-Cenomanian Events, there is a signifi (1996) interpreted the Amphidonte Event cant microfacies change from calcisphere as a shallowing episode within the subse dominated sediments to coccolith micrites quent highstand. KAPLAN & GALE (in prep.) vdth only a small foraminiferal content. can demonstrate, on the basis of bed Carbonate values range from 96 to 98%. stratigraphy, that the highest parts of these These generally poorly fossiliferous beds highstand deposits are missing due to the constitute the so-called "Arme erosive phase at the sequence boundary rhocomagense-Schichten". They display a marked by the facies change. rather inconspicuous rhythmicity ex pressed as an alternation of thick, massively Rotplaner: The Rotplaner succession is bedded limestones and very thin marls. thicker than the correlative sucessions in Two event occurrences of oysters within the Lesse Syncline, but the same subdivi this succession constitute 1) the sion into the pre-pJen us, plen us and post Py cnodon te Event, 2) the Amphidonte plen us sequences can be recognized. The Event. succession includes thin intercalations of The Py cn odon te Event comprises a marl black shales, carbonaceous marls with fish rich in small pycnodonteine oysters, some debris known as the "Fischschiefer" and two with valves associated. At this horizon else event beds with inoceramids including where are found Inoceramus pictus, I. Mytiloides hattini and inoceramids belong atlanticus and the top Middle Cenomanian ing to the pictus group. These inoceramid zonal index Acanthoceras jukesbrownei. events indicate the approximate position The marl grades up into a massive lime of the Cenomanian/Turonian boundary. stone bed which correlates with the The Violet Marl marker horizon probably Nettleton Stone of eastern England and the corresponds to the acme occurrence of "Rauhe Bank" of Buren in Westphalia (see My tiloides in the middle of the Mammites OwEN 1996). At Wunstorf and Langenstein, nodosoides Zone in the Anglo-Paris Basin. the event is underlain by an interval with Mytiloides valves encrusted by serpulids 45 (Filograna avita), recorded from just above cuvierii and /. apicalis and it has yielded a the Violet Marl at Sohlde but not from here, single specimen of Collignoniceras provide a link to the Anglo-Paris Basin. woollgari. In contrast to other localities, the The upper unit of the tripartite plenus Bed overlying M0 (or MTeuto of the Teutoburger has yielded several specimens of Wald), is represented by two brick-red marl Actinocamax plen us and a large layers. Pachydesmoceras denisonianum is inferred Finally, it should be mentioned that the find to have come from the lower part of the of one loose specimen (presumably from bed (see DIEDRICH 1996). WoOD & MORTIMORE the facies change RotpUi.ner to red/ green ( 199 5) have discussed the correlation of alternation; Fig. 2 7) of M am mites the plen us Bed with beds 3 and 4 of the nodosoides (coil. juoENHAGEN) is of consid plen us Marls of southern England. The cor erable importanceas it proves the presence relations presented by ScHbNFELD et al. of the nodosoides ammonite Zone at this ( 1991) are incorrect. There is a significant locality. non-sequence on top of the plen us Bed. There is a thickening-up sequence References: BADAYE (1986); BARTELs (1993); (highstand systems tract?) of calcisphere BRETT & SEILACHER (1991); BRONING et al. limestones below the White Boundary Bed, ( 1987); DIEDRJCH ( 1996); DITCHFIELD & MARSHALL which is itself a coccolith limestone. There ( 1989); ERNST & REHFELD (in press); ERNST et is a major hiatus at the base of the White al. (1979); ERNST et al. (1996); GALE (1995); Boundary Bed, which includes the HoRNA (1996); jEANS (1968); KAPLAN & BEsT hercyn icus Event of Westphalia. The White (1985); KAPLAN & GALE (in prep.); 0WEN Boundary Bed contains small ln oceramus (1996); B ZYNSKI ScHbNFELD Ro AS et al. (in press); et al. (1991); WooD & MORTIMORE (1995). 47 2. 7 Salzgitter-Salder quarry tions in Lower Saxony. Because of the fully (Figs. 30-33) exposed succession and, particularly in the (by C.]. Wood & G. Ernst) higher Turonian and Lower Coniacian, the enormous richness in inoceramids and Location and grid reference: TK 25, other macrofossils, the Salder quarry pro 3827 Lebenstedt-West, R: 3591000, H: vides a key section in the development of a 57777 5. To the south of the Autobahn 39 biostratigraphic framework. The succession between Braunschweig and the Autobahn can be subdivided by means of numerous junction Salzgitter near the exit to litho-, tephro- and ecoevents, which to Salzgitter-Salder, on the NE flank of the gether permit excellent correlation with Lichtenberg Hohenzug. other European localities. The highly fossiliferous Turonian/Coniacian boundary Stratigraphy: Jamarcki Zone of the Mid succession with its closely-spaced event dle Turonian up to the contact with the bundles appears to have no obvious hia Emscher Marl in the deformis Zone of the tuses or condensation and is unusual in this Lower Coniacian (Fig. 30). respect in comparison with all other Euro pean sections, except for the Vistula valley Tectonic setting: The tectonic setting is section in Poland. In view of this, the Salder complex and its interpretation is contro quarry was proposed as an international versial. The quarry is situated in the area stratotype section for the lower boundary of intersection of three major inversion of the Coniacian stage by KAuFFMANN et al. structures, the NW-SE trending Salzgitter (1996). Hohenzug, the Rhenish-trending Wendenburg fault-zone with the Broistedt Lithofacies and lithostratigraphic salt structure at its southern termination classification: On the basis of carbonate and the E-W trending Lichtenberg content, RAsEMANN ( 1984) distinguished six Hohenzug (Hohenassel) structure. Allthree different lithologies from limestone (K) to structures may have influencedthe degree marl clay (MT). In the Middle and lower of subsidence in the Salder area and the Upper Turonian, the more calcareous cat resultant thick Turonian and Lower egories predominate, while the more clay Coniacian sediments. It can be inferred that rich categories take on an increasing im a marginal trough developed in front of the portance in the higher Turonian and Lower Lichtenberg block and its extension into the Coniacian (GrauweiE.e Wechselfolge). No Salzgitter Hohenzug structure and that ad analyses are available for the lower Middle ditional salt migration from the Broistedt Turonian, but this part of the succession is saltplug took place. also more argillaceous. The microfacies has The strata in the quarry are steeply inclined hitherto been investigated only on the ba as a result of the uplift of the Lichtenberg sis of spot samples, or in limited parts of block and dip at ca.70o NNE. There are nu the SUCCeSSiOn (SIEHL in LANGHEINRICH & merous, mainly antithetic faults, but PLESSMANN 1968; RASEMANN 1984; KROGER displacements on these are small and do 1996). Calcispheres constitute a relatively not hinder correlation of the beds. The time high proportion of the rock throughout, of the inversion coincides with reaching 20% on average in the higher Subhercynian tectonism, in particular the Upper Turonian, while the foraminifera and Early Coniacian Ilsede Phase. 2.5 km to the other bioclasts represent only a small per W of Salder, in the Autobahn section N of centage (calcisphere packstones). The Salzgitter-Lichtenberg, the Cretaceous micritic matrix is largely composed of strata are vertical or even slightly over coccoliths. turned. The argillaceous limestones and marls are highly bioturbated, with complex, second General remarks: The 750 m long lime arily extremely compacted ichnofabrics. stone quarry of Fels-Werke Peine Salzgitter The compaction rate was estimated by GmbH lies parallel to the strike and exposes lANGHEINRICH & PLESSMANN ( 1 968) tO have re a ea. 220 m thick well-bedded succession sulted in a volumetric loss of 25%. They of carbonate rocks. The thicknesses of vir attributed this loss to pressure solution, tually all the strata! units are significantly which caused the original pore spaces to greater than in most other correlative sec- be completely filled. This compaction is also 48 Substages Faunal or Blozones Events c. -s tl ••••••.•••••••••••••• !g - - e -- Lower - Coniacian C. inalnstans t:?--ec-ent l o�- Ea£1eo.w11 :::J � - eao..w (j -- Eaoowr< I C. rotund.nJS =-�-- i € ea.-. C. W811.-:· 1.9 �· � 11' ...��� ...... €!>�--· · r:s-d...... M. scupinr -=--...... I ""'"'22- M M 2e; "Or_. @> D-- EaJo,wnQ """" M14·M20 """-r M10-M12 160 1----""' ""'"' MOb 1 50 ��:-•52� .- -- ' I===� G Upper 140 TF ' Turonian 130 � _ _ ._, \'":) \.)sr.r.....:e . Hortron M.I. CDSteltstus s. I. + 120 S1Tia1I:ICOriCO llfnafDt:orlo8r 110 .....i� Q;;t;,i�S... ·; .. •-•�M E I I 100 TE ---_ · 90 ro2 � '· ::;0� 0 Unit 3 (Grauwei�e Wechselfolge): The echinoids also tend to be concentrated This unit was established on the basis of at particular horizons. In addition to the the more or less rhythmic alternation of regionally correlatable Micraster Bed over (ERNST 1979) limestones and marls et al. and lying tuffs TF and TG (Micraster Event), there was more precisely delimited in an event are event-occurrences of Sternotaxis, stratigraphic framework by Wooo et al. Micra ster cortestudinarium and of an (1984). Salder is the type locality for this undescribed species of Micraster unit. On account of its wide lateral extent (Isomicraster) sp. The predominance of in Lower Saxony and Westphalia, this rhyth particular echinoid taxa in these events is mic unit provides the key to the approxi of biostratonomic interest. mate localisation of the Turonian/ Coniacian boundary in poorly recorded or Middle Turonian: Only the higher part former, now obliterated, sections, as well of this substage, comprising ea. 40 m, is as in records of shaft successions and exposed at present. The greater part of the wireline logs of boreholes. The rhythms Middle Turonian succession below a marly display a distinct thickening-upward pat layer, until recently incorrectly considered tern. It remains unclear whether or not the to be the tephroevent tuff T was not yet c• rh ythmicity is orbitally controlled. These accessible at the time of the investigations questions and other problems relating to by RASEMANN ( 1984) and by WOOD et the Grauwei�e Wechselfolge should be al.( 1984 ) , but was exposed only later as the shortly clarified from the results of current quarry was extended to the south. Conse research by the Diploma students B. KRbGER quently, only limited and poorly horizoned and T. jbRDENs-MOLLER (FU Berlin; Figs. 32, macrofossil data are available for this in 34). terval. The inoceramid assemblage exhib its an increasing proportion down-section Event stratigraphy and fauna: The of small to medium-sized, weakly sculp Salder succession can be readily subdivided tured Inoceramus cuvierii with ln oceramus by means of numerous litho-, tephro- and apicalis. However, at the base of the sec ecoevents (Fig. 30, 31 ). The tephro- and tion, there is an event with inoceramids some of the litho- and ecoevents, in par exhibiting strong tendencies towards ticular, permit an exact correlation with lnoceramus lamarcki so that it remains coeval successions elsewhere. With only a unclear whether or not the boundary with few exceptions, all the events included in the underlying apicalis/ cuvierii Zone has the general NW German event scheme been reached. The basal beds certainly still (ERNST et al. 1983) for this part of the suc lie significantly above the level of the Wei�e cession are recognizable at Salder. Grenzbank which, in condensed sections, The closely-spaced event framework and marks the boundary with the lower part of the detailed lithostratigraphic section al the Turonian and the Lower Rotplaner. The low accurately horizoned, bed-by-bed col succession can be subdivided into several lections to be made throughout the succes sequences on the basis of differing carbon sion. Near the Turonian/Coniacian bound ate content and varying bed thicknesses ary, there are extensive bedding-planes (the beds are predominantly thin-bedded). exposed from which fauna! assemblages The equivalent of the Upper Rotplaner is and populations of individual species can characterized by a ea. 3.5 m thick calcare readily be collected. From this level up to ous marl with slump structures. the beginning of the Emscher Marl, macrofossils are extremely abundant and Upper Turonian: The Upper Turonian taxonomically relatively diverse. This ap at Salder is extremely thick (140 m). The plies particularly to the inoceramids and, great diversity of inoceramids permits the to a lesser extent, to the irregular echinoids subdivision of the Upper Turonian substage and the brachiopods. In the Turonian/ into at least four inoceramid assemblage Coniacian boundary succession there are zones. The limits and fauna! characteris two beds with the interregionally impor tics of these zones were documented by tant index bivalve Didymotis. Ammonites, ERNST et al. ( 1983) in general terms and, in mostly heteromorphs, are relatively un the specific context of Salder, by RAsEMANN common. They tend to be restricted to par (1984) and by Wooo et al. (1984 ). However, ticular beds, e.g. the Hyphantoceras Event. recent as yet unpublished work on critical so events. marker honzons symools and remarks UK7S 1somrcraste1 1\181'11 _,. Mllt73 , ,, ... CJ hm•1a-.�"'*101"101o 1,111(71 1-tl many . .,. 10 MICfiiSI9r limestone .... cCW"esrucMarrumevent -·· 0 - 9 lhrnlmesti:W1ewrtn man Se l.l'oruan �-· ....,., layers ..... T I sensuSenonlan Tu Doundary ...�. -�� FrenchaUli'ICI"t mattyIITIItSIOne " .... c=J � � .. --� � ' ..."" ., ...... "' -·· E " , &\ """... ., ln'lll..., r�Wrt. ,..,.,.,... '"'" .5.., - "' -·· .., '"'" K ''"""'lOne"- CaCOJ) g." ..W$-1 !' " (95--100 mK ""'"' .. ,., ...... �us -even: -- t.lt�l-dl' @ (85-95 GaCOJ) :s 'f11181181Sl1ott«!$l$ � @ � II'II( SIIt-d �IS -8\Ient ... ma ..1'!..7.-c M'T(15- 3manyd5 " CaC03)a; ·INen! IN(·� 1-tl � :,��us... �=� �fLSIS - INII"'I II WK 431·� B tf'llnman layer 12 cm) u.�•l ...c ' MK•' dllhrlclmltker "" '"'"""' CC 13 B 6aooooo8oundary according !0 the • KM •II '" nan�l booehronol.,..!': cc 13/14. ·�> 0tayrn01rs cvonl I lP ·�"' � M SCtJpdfl e1 a!'l' Klol 3&b '' E: a; 0> MK37 1-I ScsDIHres scupm1 JoecJmgswaiMrtSIS " i 8 -· WK l!o- cl:§ "" ' @ Sc.at:mttes cr.01/11'18 ml(lJ•tl �1{3} I 31. Detailed litho- and event stratigraphy of the Turonian/Coniacian boundary succession of the pro Fig. posed international standard section at Salzgitter-Salder (after Wooo, ERNST & RAsE�tANN 1984). inoceramid assemblages from eastern Eu assigned by Wood et al. ( 1984) to the sin rope has necessitated significant modifica gle broad species concept of lnoceramus tion of the inoceramid zonation then used. aff. fre chi, are now considered by TROGER & The numerous eco-, tephro- and lithoevents WALAszczYK (in press) to be unrelated to the in this substage provide a relatively simple true (highest Lower Coniacian) I. fr echi. In key to the location of the approximate po their view, the two morphotypes should be sitions of the zonal boundaries in the field. referred to My tiloides scupini and M. The Mytiloides scup1m (formerly herbichi respectively. The M. scupini Zone Inoceramus aff. fr echi) Zone comprises a begins at TF and extends up to just below 50 Didymotis ea. m succession within which a signifi the 11 Event. It is thus approxi cant lithofacies change takes place from mately co-extensive with the uppermost massive limestones to the rhythmic marl Turonian Prionocyclus germari ammonite limestone alternations of the GrauweiE.e Zone of KAPLAN & KENNEDY ( 1994), which be Wechselfolge. The inoceramid fauna of this gins 2 to 3 m above the Micraster Marl and zone is relatively sparse. The two eo-occur terminates just below the Turonian/ ring inoceramid morphotypes that collec Coniacian boundary. tively characterize this zone, provisionally Only the stratigraphically most significant 51 events and marker beds ft1nt layer C.mconstans Maaster COttestudinsnum event l'lannoverensis event / waltersdottens's event '> wa"er.; - C1orfenstsOldymolis hannoverensts 11 /C event f \ - Dldymotts I I M. scupm1 ,_,, �- ·� .,- :5? l\ \ \ I t r . �-----. i I < I • .--- \ \ > \ / � "- \\ r \ .. 3 2. Carbonate content and semi-quantitative analysis of foraminifera and calcispheres in the Upper Fig. Turonian-Lower Coniacian succession of Salzgitter-Salder (after KROGER 1996 and jbRDENs-MOLLER 1996). events in the Upper Turonian are discussed Didym otis Event. Further details of these here: 1) costella tuslplana Event, 2) ME and the other events as developed at Salder event-bundle, 3) Hyphantoceras Event, 4) are to be found in Wooo et al. (1984). Mytiloides incertus Event, 5) event-bundle The costellatus/ plana Event is character tuff T marl MG and Micraster Marl, 6) lower ized by the mass eo-occurrence of thin- P 52 shelled inoceramids of uncertain affinities marl Me, previously considered to be a tuff (including the eponymous group of comparable with TF' has now been shown /noceramus caste/la tus) together with to be a detrital marl (WRAY 1995; WRAY & Stern otaxis plana. Associated with the Wooo 1995). Work in progress suggests that guide-fossils are sparse A/locrioceras, tuff TF is the highest tuff in the Turonian Sciponoceras and Scaphites cf. diana, as tephrostratigraphic scheme. The Micra ster well as Infulaster excen tricus. Following its Marl event is characterized by the occur first appearance in this event, I. costellatus rence of advanced Micraster of the bucailli does not reappear until the overlying zone. lineage near to the marl with a distinct con The event is restricted to a thin, clearly centration in the marl itself. delimited bed intercalated between other The lower Didym otis Event (DJ) is charac wise relatively poorly fossiliferous lime terized by the common occurrence of the stones; it can be readily located by its posi thin-shelled bivalve Didym otis in a 0.45 m tion some 6 m beneath tuff T marly limestone (MK 39) associated with 01 • The ME event-bundle comprising the con Inoceramus lusatiae, Mytiloides herbichi spicuous 0.3 m thick marl ME with its asso and M. scupini. Didymotis has a virtually ciated underlying tuff (TE) and overlying worldwide distribution and is of great thin marl ME-chen can be traced throughout biostratigraphic importance for long-range Germany and is the key to the correlation correlation. A lower Didymotis occurrence between thick, clay-rich successions such (designated 00) has now been recognized as Salder and relatively thin, carbonate-rich in bed 19 (KRbGER 1996), this occurrence platform equivalents as in the Sohlde quar may correlate with an event bed with rare ries in the nearby Lesse Syncline. Didymotis sp. in the lower part of the The Hyphantoceras Event (ERNST et al. 1983; Grauweige Wechselfolge at Hoppenstedt, DAHMER & ERNST 1986) has a thickness of which was formerly believed to be equiva about 6.5 m at Salder, with its base approxi lent to one of the main Hyphantoceras mately 17 m above marl ME. The event is Events on the basis of its ammonite and named after the occurrence of the inoceramid fauna. heteromorph ammonite Hyphantoceras re ussianum. The base of the event is typi Turonian/Coniacian boundary suc cally marked by a 2 m fining-upward se cession: This comprises an event-bundle quence of coarse-grained, bioclastic sedi of three very closely-spaced bioevents ment containing inoceramid shell frag within less than 0.5 m, which spans the Didymotis 2) ments, smooth-shelled brachiopods and stage boundary: 1) 11 Event, ammonite fragments. Immediately above C. waltersdorfensis waltersdorfensis Event, the top of this basal unit the first 3) Cremnoceramus rotundatus Event_ Hyphantoceras Didymotis fragments appear (first The 11 Event (bed 45) comprises Hyphantoceras-acme). The second a near-monospecific assemblage in lime Hyphantoceras-acme lies ea. 2 m above the stone preservation of small inoceramids first one and has a thickness of ea_ 3 m. referred by Wooo et al. ( 1984) to small The development of the Hyphantoceras Cremnoceramus waltersdorfe nsis Event in Salder does not correspond to the hannoverensis, but now considered "normal development" (DAHMER & ERNST (WALASZCZYK & Wooo in prep.) to be 1986), since the thicknesses found here are conspecific with C. waltersdorfensis three to four times those usually attained. waltersdorfensis. The inoceramids are as This is probably connected with the greater sociated with common Didym otis cf. degree of subsidence and the intercalation costatus. waltersdorfensis waltersdorfensis of allochthonous sedimentation. The C. The Mytiloides incertus Event has not yet Event (bed 46) is a near-monospecific as been proved in Salder, but its apparent semblage of the eponymous inoceramid absence is perhaps more due to collection associated with rare large Didymotis. The failure than to an actual non-sequence. inoceramids are preserved in mar! with the The bundle of the three closely-spaced shell and the two valves in association, but events tuff TP marl Me and the Micraster are predominantly considerably com Marl (Me) comprises an excellent marker pressed. with wide regional extent (Wooo et al.1984). The Cremnoceramus rotunda tus (sensu On the basis of rare earth geochemistry, TRbGER non FIEGE) Event (bed 4 7) is a near- 53 ·- - ...... ·� ·--�-...... loalllonthe of outcrops - Fig. 3 3. Correlation of the Upper Turonian M. scupini Zone between Lower Saxony and Westphalia. monospecific assemblage of the eponymous were accessible, and were cursorily docu inoceramid in limestone preservation.This UTIGAM (1962). mented by BRA The highest marks the first appearance of C. rotundatus, 40 m fell in the Volviceramus koeneni Zone, which, following the recommendation of i.e. basal Middle Coniacian in the sense of the Brussels Symposium 1995, is the unique inoceramid stratigraphers. boundary marker for the base of the The part of this succession that is still avail Coniacian stage. The base of the stage is able can be readily subdivided consequently shifted upwards from the lithostratigraphically using the numerous Didym otis 11 Event to the rotundatus Event, marl-seams and the two flint beds at the from which it follows that the two main top of the section. The succession can also Didym otis Events belong to the terminal be readily subdivided using event Turonian. stratigraphy. In addition to some This sudden appearance of Coniacian inoceramid fl ood-occurrences, two inoceramids in closely-spaced event-beds echinoid events, the Micraster is one of the most striking features of the cortestudinarium and the Isomicra scer Salder succession. Forresteria (Harleites) Events, can be distinguished. The petrocoriensis, the index of the base of the biostratigraphic significance of the Coniacian for ammonite stratigraphers, has Didym otis 11, waltersdorfensis never been found in Salder, or anywhere waltersdorfensis and ro tundatus Events else in Lower Saxony, but occurs signifi have already been noted. Other inoceramid cantly above the base of the stage in events here comprise the waltersdorfensis Westphalia (KAPLAN & KENNEDY 1994). An hannoverensis, inconstans and deformis unequivocal Lower Coniacian ammonite ecoevents. The hannoverensis Event marks fa una (Scalarites turoniense, Neocrioceras a level of significant increase in inoceramid paderbornense and Scaphites kieslings diversity and speciation, as does the wa ldensis kieslingswaldensis) first appears lsomicraster Event (WALASZCZYK & Wooo in in Salder at or a little below the Isomicraster prep.). The latter is named from the com Event (bed 75). mon occurrence in bed MK7 5 of a relatively large, rounded Micraster (lsomicra ster) sp. Lower Coniacian: At present only SO m and likewise appears to offer good correla of Lower Coniacian are exposed. Previously, tion potential within a relatively restricted 65 a fu rther m of the overlying succession area (e.g. Floteberg section). 54 References: BRAUTIGAM (1962); DAHMER & (1996); LANGHEINRICH & PLESSMANN (1968); ERNST (1986); ERNST et al. (1979, 1983 ); RASEMANN ( 1984); TROGER & WALASZCZYK (in jORDENS-MOLLER (1996); KAPLAN & KENNEDY press); WALASZCZYK & Wooo (in prep.); Wooo (1994); KAUFFMANN et al. (1996); KROGER et al. (1984); WRAY & Wooo (1995); WRAY (1995). 55 2.8 Sohlde quarries (Figs. 34-36) level fall. These sedimentary disturbances (by G. Ernst & C. ]. Wood) were thought to terminate at one of the more important sequence boundaries, UZA Location and grid reference: TK 25, 2.6/UZA 2.7, which is marked by the base 3827 Lebenstedt-West, R: 3585400, H: of the Wei&e Grenzbank (White Boundary 5783935. From some 15 quarries situated Bed). However, we consider that these phe south of Sohlde and along the road between nomena do not result from a single cause, Sohlde and Barbecke, three (the Loges and particularly as comparable processes at Damman quarries) are described in detail. other sequence boundaries are either not Together they provide a more or less com observed or are represented only to a lim plete composite section through the Sohlde ited degree. In our view, these can be at chalk. tributed to tectonic pulses during the mid Turonian, forerunners of the later main Stratigraphy: Middle Cenomanian Subhercynian tectonic phases, which initi prim us Event in the Witt quarry (also ated possible tectoeustatic processes. A new known as "Sohlde 1000") to the Upper working quarry in the vicinity of the Turonian Grauwei&e Wechselfolge. Dammann plant actually shows that the Wei&e Grenzbank itself has been frag Tectonic setting: The Lesse Syncline lies mented into blocks by sliding processes, at the southern margin of the Gifhorn which contradicts HILBRECHT's model. The Trough. Its structural history was largely culmination of these activities must also be influenced by salt movement of the placed at a stratigraphically higher level Broistedt saltplug and of the Luttrum and than hitherto thought, somewhere beween Westerlinde salt horsts in the Lichtenberg tuff Tc and the costellatus!plana Event, Hohenassel structure (BAuERLE 1980). since-particularly at the level of the Upper Acccording to VINKEN (1971 ), halokinetic Rotplaner-comparable submarine sedimen activity of the Mblme and Gro&-Ilsede salt tary anomalies are to be found not only in structures to the north may also have the Sohlde area, but also in some other com played a role. The Luttrum and Westerlinde parative sections. salt plugs already exhibited some degree of activity during the Early Cretaceous, but Lithofacies, lithostratigraphy and their infl uence on Cenomanian and events: The succession exposed by the Turonian sedimentation was quite minor Dammann and Loges quarries can be sub (slight reductions in thicknesses towards divided into four main lithostratigraphic the salt structures). A similar development units (Fig. 34): is seen in the case of the complicated struc Upper Cenomanian Limestones ("Arme • tural history of the Broistedt salt plug rhotomagense-Schichten"), ea. 16 m to ( B-\ liEI\LE 1980; RAuFuss 1985 ). The thick the base of the Loges quarry, nesses of the lower part of the Upper Cre Rotplaner (ea. 32m), • taceous in the foredeep situated in front of Wei&planer (or Lower Limestone Unit; • the Broistedt salt structure are significantly 50m), greater than those in the Sohlde area of the Grauwei&e Wechselfolge (ea. 15 m up to • Lesse Syncline. This provides evidence for the top of the Dammann quarry). strong synsedimentary control of the depositional area, which is reflected to a Cenomanian limestones: The upper limited extent by lateral thickness varia Middle Cenomanian with the Pycn odonte tions and the development of hiatuses in Event is accessible only in some of the west the Sohlde chalk. ern quarries of the Sbhlde chain of quar Syndepositional tectonism, expressed by ries. As the result of the establishment of a intraformational slides, rotational slumps dump for construction rubbish in the most and related phenomena, were described by westerly Witt quarry ( = "Sohlde 1 000" of HILBRECHT ( 1988) from the lower part of the HILBRECHT & DAHMER 1994), the lower Middle Turonian of some of the Sbhlde quarries. Cenomanian prim us and Mid-Cenomanian One year later, HILBRECHT ( 1989) attempted, Events, which were formerly exposed along without applying tectonism, to explain the side a fault, are becoming progressively same phenomena by invoking pore-water covered. The succession here was docu over-pressure resulting from eustatic sea- mented in detail by DAHMER ( 1986) and also 56 remarks lithology and event sequence hiati and sub m on facias stratigraphy stratigraphy + condensation stage lithology 90- ....---- ....• .... F 'Grauwei8e Wechse�olge" c ctS c hiatus ? hardgrounds or conclensalion 0..... < ::J hiatus ? 1-- ...... < ..... - -- flints + ...... condensation 60 ...... F• Q) Ortlirhynchisfacies a...... a. ME +MEdw'l ------condensation ::::> - - - TE ! flints 50 F -0-:1- CGnulus- .Conulus(Woltwiesche) facies ...... l TD2 40 rsr :.: slumpings LST ...... - __ - -.-01 l oJr- aJSf8lalus JpltVlsmarl ss!l marl layers ·· . hiatus ? r- :_, - :J -...... -.. slumpings < flints condensation 30 • • - • • • HST --l,_j -··- C'.a1uful.F23 � j - TST : ------: ---,: upper : SB .i_ [; ROipliner i } -�� �ump1ngs j TST middle l Rotplilner l R i :i � 10 )... --: hiatus �- c R _j e 0 : 2 .SB : 3 h18ti _ ·- ---: 'Arme i j rhotomagMse j l Kalke' ! ;·_T:;J: : � .. 34. Generalized standard section of the Upper Cenomanian to Upper Turonian of the Sohlde area. Fig. treated by ERNST et al. ( 1992 ). The tent of calcispheres and foraminifera. Pycn odonte Event, i.e. the boundary event About 3 m above the Pycnodonte Event at the base of the Upper Cenomanian, is another oyster event occurs, the lower developed here as a marl bed rich in the Amphidonte Event. The extent of the hia oyster Pycnodonte within rather uniform tus in the vicinity of the facies boundary at white limestones. It has also yielded rare the top of this succession has not yet been Inoceramus ex gr. pictus and a whorl frag calculated in the context of the bed ment of Acanthoceras jukesbrownei. The stratigraphy developed by KAPLAN (unpub traditionally named "Arme (poor) lished) in the Teutoburger Wald. rh otomagense-Schichten" (so-called from their extremely poorly fossiliferous char Rotpla.ner: The Rotplaner succession in acter), overlying the Pycn odonte Event in Sohlde can be subdivided into three units, the Loges quarry, do not differ in any way the Lower, Middle and Upper Rotplaner from those exposed at the Baddeckenstedt (Fig. 34). The Lower and Middle Rotplaner quarry. The microfacies comprises a rather are separated by a conspicuous, ea. 2.5 m pure coccolith rock with a subordinate con- thick bed of white limestone, the so-called 57 Wei&e Grenzbank. Sohlde is the type local pictus bohemicus and small brachiopods ity for this widely traceable event. The such as Orbirhynchia wiestii and Wei&e Grenzbank is overlain by a conspicu Mon ticlarella jefferiesi. The complex plenus ous red marl bed (the so-called T which Bed with its underlying upper Ch ondri tes 0 ) , was originally interpreted by BRAUTIGAM Event constitutes an outstanding inter-re ( 1962) as a tuff, and was consequently gional event, which can be correlated in given the symbol T. It is probably a lag detail as far as Westphalia (ERNST et al. 1992) deposit and represents a significant hiatus. and even to England (see discussion by The Wei&e Grenzbank and the T0 together WooD & MORTIMORE 1995 ). constitute a conspicuous marker sequence, The post-plen us succession is more com which is represented in the Teutoburger pletely developed in the western quarries Wald by a comparable bed of limestone of the Sohlde chain than it is in the eastern overlain by a thick marl, the so-called Mnuro quarries. This is documented by the inter sensu KAPLAN. Both the T and M o have calation of a basal green succession, includ 0 TEUT been shown on the basis of rare earth ele ing the "Fischschiefer" (Fish-shale) event, ment analysis to be detrital rather than which can be correlated to Baddeckenstedt vulcanogenic marls (WRAY & Wooo 1995; and other localities (ERNST et al. 1984 ), and WRAY et al. 1996). The Middle and Upper falls in the uppermost Cenomanian. The Rotplaner are likewise separated by a pale first really overlapping event of this se coloured bed of marly limestone (bed 17). quence on the north-western margin of the In comparison to Baddeckenstedt (ea. 24 Lesse Syncline is the so-called Bunte (vari m), the Lower Rotplaner at Sohlde is mark egated) Mergellage (DAHMER 1986; HILBRECHT edly condensed (ea. 11 m). It comprises & DAHMER 1994 ). This event marks the en three sub-units, the pre-plenus succession, try of shell detritus from the inoceramids the plen us Bed and the post-plenus succes Mytiloides ex gr. mytiloidesl Jabiatus. The sion. Despite condensation, the pre-plenus overlying thin limestone bed at the Sohlde succession together with the plen us Bed can 1000 quarry yielded a single specimen of be satisfactorily correlated with the same the basal Turonian zonal index ammonite beds at Baddeckenstedt, although there are Wa tinoceras devonense. The Bunte some differences in detail. In the Sbhlde Mergellage can therefore be used as a quarries, the pre-plenus succession exhib marker to identify the approximate posi its lateral variation in both thickness and tion of the base of the Turonian in the development, and shows evidence of occa Sohlde area. However, the truestage bound sional resedimentation (HILBRECHT & DAHMER ary lies significantly lower in less con 1994 Chondrites ) . Two event-beds are densed successions. present, the lower corresponding to the Above this bed, there is a marked change extinction datum of Rotalipora in style of sedimentation, characterized by greenhornensis and the higher to the (lo repeated reworking during high-energy ca l?) last appearance datum of Rotalipora episodes. Winnowing resulted in an in cushmanni (EHNsT et al. 1984). The upper crease in the proportion of shell debris and event represents the original Ch ondrites calcispheres. The microfacies changes from Bed of ERNST et al. ( 1983) and is situated at wackestones to packstones. Guttercasts, the boundary with the plen us Bed. The calcisphere-filled scour channels and green plenus Bed at Sohlde and neighbouring lo coloured (reduced) high-angle shell debris calities is a complex, tripartite bed with document a distal tempestite facies. The three highly bioturbated separation planes gutters and scours contain well preserved, (HILBREC:HT & DAHMER 1994 ). At the top and, complete valves of Mytiloides Jabiatus, typi less distinctly, at the base of the bed, there cally in "convex-downward" position. This is an hiatus marked, among other features, depositional pattern terminates at the so by reworked nodules with a greenish-grey called Violette (violet) Mergellage, an event ScHONr-ELD 1991 coating (see also et al. ) . The only a few centimetres thick, but neverthe eponymous belemnite Actinocamaxplenus less widely traceable in many N German is extremely rare, a single specimen found localities. This event marks the first mass so far probably coming from the top part occurrence of My tiloides mytiloides (the of the bed. The remaining fauna comprises lower fades-overlapping MytiloidesEvent ). small pycnodonteine oysters (abundant in The Mytiloides shells ea. 0.1 m above the the lower part of the bed), lnoceramus Violette Mergellage are encrusted by 58 .. .. u.ted) Ill r. fonmintt.ra raUoi U:Mnktonlelbenthon6c, llNiedlnon lithology celcl8phetH • • c CD !! !l and events "E �foramlnil•ra ptanktonlclbtnthonk: = llnledlnon-*•led !! .! 0% 25 so 70 80 90 100 25 so 75 100 Ill :I ::::l Ill mr------, .. 1. 18m11Citl ;; r::a.• :!!c r::a... .t :::1 - 3t - ' .. ' ' .. ' . ..c -.-- ·- I a. 0 a::.. z !. r::a. c ::::l z • 0 "a a:: "a- - - L :::1 ..c :I 1- ::E a. 0 a:: � ' ' ' _ _ ___l_ __ i ' ' · ' ' r. 1-- - ;· .------=---.--- ' i ' ' .. - .. .. : - l f ! • c l--+o--!--;F4- c- �-- � a. � ---- 0 0 .. · ...J a::.. ��-��-�--�. --+- -� '-- f-- 3: - !--�--=-- 0 ...I 1-- .. ., c: 0 z ., .. u; c .::;E Gl .. z r::a. "' < c. "' -Amptuaonteevent ""c: ::E :::1 "' 0 E z !2 w 0 u 'E 0 0 c.. Pycnoaonr• 1-- event Gl " '6 't-- "a i i ! 3 5. Middle Cenomanian to lower Upper Turonian lithology I and stratigraphy in the Sohlde area with Fig. semi-quantitative analyses of foraminifera and calcispheres (after Borrc:mH 1996). serpulids. This event probably corresponds that secondary oxidation took place in the to the Filograna avita horizon described by relatively porous sediments of the burrow GALE et al. ( 1993) from an equivalent level fills. The upper boundary of the Middle in the Anglo-Paris Basin. RotpUi.nerat Sohlde and many other locali The Middle RotpHi.ner is usually pink ties is marked by the first tuff bed (TJ. rather than red-coloured, and it exhibits However, the red coloration may extend a extensive bioturbation ( Th alassinoides). little bit higher. The sucession around Tc is The colour is predominantly restricted to additionally characterized by a geographi the Th alassinoides burrow-fills, which pos cally widespread Inoceramus lamarckil sibly document tubular tempestites sensu cuvierii Event. TEDESCO & WANLESS ( 1991 ). It is also possible The Upper Rotplaner is red-coloured in ------59 .. calclspherea fon�minifera r.Jtlos (plank1onlc/benthonlc, kHiedlnonkHied .. · · "' en toramlnllenll .!!.. !I lithology and events • planlllon•c:lben1honlc; :...... • kHiedlnon·ll"led ::J "' ·c: � :1 ..Q � 0% 25 5 70 80 90 100 25 50 75 100 = 11) .. en � i ! 'ii.. l � u.. ;::.. "" ' ' · ' ;; ' 3: = ' I! -0 ' ' ' ' ' ' ' ' .._ . __ c; ,------7-, -- �-�--� .. ! : ! ' : : __ : __ _ , _! ' J . ...., -- � � r - -- 1--+-+-�---- - : -- - T- 1 - z - . [ : � ------c( -:- : � � -� .. - ��=*=*=�� � - z c. . .,.. T 0 ���� -�r c. � - a: _.. ::l _ ....� - ::l 1--+-+- - - !__ � ___ 1- ..� ,]"""""' --�=- .-; - I c ��=±=�� ,:�=- '------}.:_ _; --� �I ...... --- - -�· ' : "" ; Q. .. - · r� ;; . . r- ;:: .. 1 .. �; --- . -eo T �--- � -=----- · i _-_i__ i------· - : ...._ , _ _ _ _ � i _ ------! --t -=.....:, ' '; ...... '� --= T - : � ! r- -· -- · 1 ------==' ·-� �----,._of=- L__ --1 -== �. =--= : · � Upper Conu/u$ even: l ·:__ !_ __· ��: -.--� -· i Fig. 36. Upper Turonian lithology and stratigraphy in the Sbhlde area with semi-quantitative analyses of foraminifera and calcispheres (after BoTTCHER 1996) only a few of the Sohlde quarries, which Wei.&planer: This Upper Turonian succes clearly reflect the shallowest parts of the sion is significantly more calcareous than depositional area. The red-coloured beds the beds below and is preferentially ex are mostly replaced by grey marls of vary ploited by the quarry companies for this ing abundance. At the top of this unit and reason. The microfacies comprises a rather at the base of the overlying Wei.&planer, an monotonous white calcisphere-rich event with Sternotaxis plana and Con ulus coccolith micrite. Four event-bundles in the subrotundusmarks the first echinoid event lowest, middle and uppermost part allow following a long interval without such the unit to be subdivided and permit wide events and even virtually without echinoids ranging correlation: 1) flint horizon F23 to in general. tuff T 2) marl-bed T 02 to marl-bed M 3) nl' E' 60 flint horizon Fx and Hyphantoceras Event, to Tuff Tn1 and represents the second of 4) tuff T to Micraster Marl. the tuffs described by & BRAUTIGA�I r 00RJ\ In sequence stratigraphic terms, the event (1959; their Tuff B). The 0.3 m thick mar! bundle F 23 to Tn1 corresponds to the late bed M[ is the most striking and perhaps highstand of one sequence and the the geographically most widespread marker lowstand and transgressive systems tract horizon of the lower part of the Upper of the following sequence. The late Turonian. Mr is usually followed, 0.3 m highstand includes the fl int horizon F23, higher, by a thin marl bed known as the which is situated near the base of the ME-chen· Both these marls have been likewise Wei�planer and for which Soh! de is the type shown on the basis of their rare earth ele locality. It consists of several layers of thin, ments to be detrital rather than commonly white-striped tabular flints, in vulcanogenic marls (WRAY & WooD 1995). addition to sporadic vertical elements, in a The interval between the marls contains an unit of thin-bedded limestones about 1 m echinoid event comprising thin-tested thick. This flint event can be traced to the forms such as Infulaster and/or Sternotaxis. eastern Teutoburger Wald (WRAY & WooD In some comparative sections in Lower 199 5) and is in all probability represented Saxony and Westphalia (e.g. Floteberg, in eastern England by the so-called Ferru Bielefeld etc.), Infulaster occurs predomi ginous Flint (see WooD et al. 1984). It is nantly or exclusively at this level. An addi absent in the marly foredeep sediments of tional, rather scattered, echinoid occur the Salzgitter-Salder quarry, although its rence lies in the region of Tr or below the position can be easily identified at a thin tuff. In the Woltwiesche quarry, ea. 2.5 km bedded limestone horizon. In the con north-east of the Dammann quarry, the densed vicinity of the sequence boundary relatively common occurrence of Con ulus is found the costella tuslplana Event, which below TE, in an intervalseveral metres thick, marks the base of the Upper Turonian. The represents the initial development of a position of the event can be readily identi Con ulus facies. fied by a marked increase in limonitized The event-pair Fx and Hyphantoceras Event sponges at the same level. The commonest falls again in the vicinity of a sequence fossils are the eponymous thin-shelled boundary. The only very weakly developed ln oceramus costellatus and related species, flint bed (Fx) lies within a condensed and together with Sternotaxis plana; the only relatively conspicuous brachiopod horizon ammonite from here is a poorly preserved which yields Orbirhynchia and small Lewesiceras sp. smooth terebratulids of uncertain affinity. The event is overlain by a thin slump hori This horizon is traceable at least in eastern zon (movement to the south ), which is fol Lower Saxony (e.g Salder, Floteberg, etc.). lowed by two mar! beds, which may well On the other hand, the Hyphanwceras belong to the transgressive systems tract. Event some distance higher, is extremely The event-bundle terminates upwards at poorly represented in the chalk facies of the conspicuous tuff bed Tn1 , which is one the Sohlde quarries and is difficult to lo of the original tuff layers (then designated cate. Its development here is quite atypi Tuff A) described by DoRN & BRAUTIGAM cal, consisting of an horizon with (1959) from the Sohlde area (see WRAY & limonitised sponges, thin-shelled Woon 1995). This ea. 0.05 m thick tuff bed inoceramids, small brachiopods and rare is divided into a lower barren part com Scaphites geinitzii. Hyphantoceras appears posed of greenish-yellow montmorillonitic to be completely absent. Either the event clay, and an upper grey part which becomes in Sohlde falls within a succession with more calcareous upwards and again yields many hiatuses, or the sparse development some nanno- and microfossils. here corresponds to a pelagic version of the The event-bundle T 02 to Mr comprises a highly fossiliferous event found elsewhere combination of various litho-events: mar! in different depositional situations (see beds, a tuff and a flint bed. T has been DAHMER & ERNST 1986). 02 shown to be a detrital marl (WRAY & WooD Once again, the event-bundle T, to 1995) and consequently has been Micraster Mar! falls in the vicinity of a se redesignated Mn. Particularly conspicuous quence or parasequence boundary. It is and most readily correlatable is the suc underlain by a succession of one or more cession TP Mr and ME-chen· Tuff E is similar hard- or firmgrounds associated with thin 61 debrites. The last appearance datum of element of the topmost Turonian In oceramus ex gr. inaequivalvis is found at Prionocyclus germari ammonite Zone. this level. The event-bundle itself comprises two thin and one 0.05 m thick marl bed in Grauwei&e Wechselfolge: This litho an interval of only 0.5 m, constituting the unit is relatively inaccessible at Sohlde and so-called "Dreiband" (triple band). The poor in macrofossils. In comparison to thicker upper marl yields advanced Salder, the marls are thinner, paler and not Micraster of the bucailli lineage and there so clearly defined. However, they all ap fore unequivocally represents the Micraster pear to be present and show the same thick Event of other localities (e.g. Salder). The ening-upward pattern (WooD et al. 1984; two lower marls were formerly identified KROGER 1996). As in the case of the lower as tuff TF and the supposed tuff "T"G re litho-units, the GrauweiB,e Wechselfolge is spectively, but rare earth element analy 50% thinner in Sohlde compared to Salder. ses (WRAY & WooD 1995) have shown that Only the lower part of the unit is exposed they are both detrital marls. The absence in the Sohlde quarries and the Turonian/ of the widely distributed marker tuff TF Conician boundary interval is nowhere ex from the triple band of the Sohlde chalk is posed. However, in the now backfilled puzzling. It is suggested that either this tuff former quarry near Barbecke, ea. 2 km east was not deposited in the Sohlde area or that of the Dammann quarry, a well preserved after deposition it was rapidly eroded (WRAY low (but not basal) Lower Coniacian et al. in press). Above the Micraster Marl inoceramid assemblage dominated by large there is a minor facies change to slightly Cremnoceramus waltersdorfensis more clay-rich sediments. The calcisphere hannovrensis was collected from sediments content increases suddenly at this level and in unexpectedly chalky facies. there is a concomitant decrease in the foraminiferal content (KROGER 1996). Spo References: BAUERLE ( 1980); BOTICHER 1996; radic clusters of Con ulus occur ea. 0.5 m BRAUTIGAM (1962); DAHMER & ERNST (1986); above the Micraster Mar I. All these charac DAHMER (1986); DORN & BRAUTIGAM ( 1959); teristics support the hypothesis that there ERNST et al. (1983, 1984, 1992); GALE et al. is a sequence boundary in the vicinity of ( 199 3); HILBRECHT & DAHMER ( 1994); HILBRECHT the Micraster Marl. There is also a signifi (1988, 1989); KROGER (1996); RAUFUSS (1985); cant change in the ammonite assemblages ScHONFELD et al. (1991); TEDESCO & WANLESS some 2 to 3 m above the marl, marked by (1991); VINKEN (1971); WooD & MoRTIMORE the occurrence in a quarry near Nettlingen ( 1995 ); WooD et al. (1984 ); WRAY & WooD in the western part of the Lesse Syncline of (1995); WRAY et al. (1996). Hyphantoceras flexuosum, a characteristic 63 Gott clay-pit near Sarstedt (Figs. 2.9 37- 5 3 ) (by ]. Mutterlose) Location and grid reference: TK 25, 3725 Sarstedt, R: 3560400, H: 5790650. The clay pit is situated about 30 km south of Hannover (Fig. 2). In 1993 the pit, which is a key section for the study of sediments of Early Cretaceous age, was closed down. Currently claystones of Barremian and Aptian age are being quarried in a new sec tion directly north of the Gott section. Tectonic setting: Northwest flank of the Sarstedt-Lehrte salt structure, about 1 km from the salt dome (Fig. 37). The beds dip at 25° towards WNW. There are several minor faults, each with a displacement of about a metre. Palaeogeography: Eastern part of the NW German Basin, about 20 km north of the Hildesheim Peninsula. The palaeogeography varied considerably dur ing the interval under discussion. In Hauterivian times a sea-way existed towards the Tethys via Poland (Carpathian sea-way) allowing floral and fauna! exchanges. The Barremian is characterized by a major re gression causing restricted conditions. No direct sea-way existed towards the Tethys, and the entire NorthSea formed a marginal restricted basin. This palaeogeographic configuration allowed for the deposition of 3 8. Sketch map of the Gott clay-pit. anoxic sediments (Blatterton,Fischschief er) Fig. and the evolution of endemic floras and fa unas. The overall transgressive Aptian is wards the west via a Proto-Channel and marked by a change of the palaeoceano Tethyan floras and faunas invaded the ba graphic setting. A new sea-way opened to- sin from the west. Stratigraphy and lithology: About 85 m of clays and marly clays are exposed (Figs. 38, 39). Strata of latest Hauterivian age (Simbirskites gottschei ammonite Zone) and Barremian age (Pra eoxyteuthis pugio to Oxyteuthis depressa belemnite Zones) are unconformably overlain by mid- to late Aptian strata (Parahoplites nutfieldiensis to Nolaniceras nolani ammonite Zones). This pit exposes the most complete section of Early Cretaceous sediments in NW Germany (MUTIERLOSE 1984, 1995; Fig. 39). About 12 m of fossiliferous clays of Hauterivian age (gottschei and discofalcatus ammonite Zones) are exposed Fig. 3 7. Geologic map of the NW shoulder of the Lehrte-Sarstedt anticline. (Fig. 39). These show typical bedding 64 I- D I Gott I Sarstedt -t- , � I ��� I � r- I !!! :; �: � 5 r 0.., .!!� J , '( c 5 3 , - ..... t-- 4 - • z c " . � 2 c � . . .. e E D 2 ! Q. 0 :! 0 "' c Q; �0. ii "' 3, Ill . '( Q C>. 8 3 • -� cl a. • 2 a. a. t- I :::> a. • :::> , -� 2 , � 2 t- , . . t f£ � ; I- . �� ..� I c :; • I .., � � ; 0 ; :;: . -;; .. :r "' c . ; a. e 2J� .1r--;t-- a. I� ' :::> � I,·� Ill � � , t- ; c. .. a. � a. " F� :::> Q 0 g Fig. 3 9. Bio- and lithostratigraphy of the Gott section. Legend see Fig. � J 40. rhythms of numerous pale and dark beds, and Chondrites beds. Beds rich in pyrite intensively bioturbated at some horizons. are common, and there are two thin These beds yield a rich micro- and Blatterton horizons. The carbonate content macrofauna (interval A in Fig. 39). of this interval does not exceed 5%. In bed The Barremian comprises about 56 m of 107 Criocera tites elegans is common. The medium and dark clays. The lithology of upper part of the Barremian is lithologically the lowermost 8.6 m (Pra eoxyte uthis pugio much more monotonous. The clay becomes belemnite Zone of the Early Barremian) is darker towards the top and several sandy very similar to those of the Late Hauterivian horizons are intercalated. Bed 197 yields (clay-marl rhythms, Ch ondrites horizons). Pa rancyloceras bidentatum. The belemnites These beds correspond to interval B in Fig. Oxyteuthis brunsvicensis, 0. germanica and 39. About 5.7 m of finely laminated 0. depressa are common. The carbonate sediments, the HauptbHi.ttertonof the Early content decreases towards the top. Barremian, were deposited under anoxic The Barremian-Aptian boundary is charac conditions. These have been assigned to terized by a hiatus, strata of Early Aptian faunal interval C (Fig. 39). The reminder and early Late Aptian age (Prodeshayesites of the Barremian (intervalDi n Fig. 39) con forbesi to Ep icheloniceras tschernytschewi sist of 41.5 m of clays and marls. The lower ammonite Zones) are missing. The latest 15 m are dominated by pale marly layers Aptian (Parahoplites nutfieldiensis to 65 Legend: tion (No. 14). The pale beds yield calcare nodules ous nannofossils of Tethyan provenance C> limeltone Calcareous Sandstone . (Nannocon us spp.). A sudden influx of . Pyrite )( nannoconids in bed 58 ( 9% of the total • .1. Bioturbelion abundance) allow a regional correlation Sand lens with bed 117 of the Frielingen section. This Ammonites 8 Nannocon us event occurs just below a ho 1�1 Belemnites rizon characterized by the belemnite Clay p Acroteuthis. The foraminifera are domi - Glauconlle m .. nated by Epistomina caracolla and E. Colours omata. Bliitterton dark grey Interval B: Comparable to intervalA; well grey oxygenated nearshore environment. The pale Tul l Hauterivian/Barremian boundary is, how red 8 ever, marked by a change of faunas and green floras. Within interval B, Boreal and en demic floras (Nannoconus abundans, N. Fig. 40. Legend of Fig. 39. borealis) and faunas (Praeoxyteuthis, Hibolites minutus) become common. These Nolaniceras nolani ammonite Zones) is rep elements mark the closure of sea-ways to resented by 19 m of clays and marls. The wards the Tethys. basal 4 m (interval E) are represented by varicoloured pale and red marls Interval C: Stagnant conditions caused by (Hedbergellen Marl), which yield two tuff restricted palaeogeographic setting re horizons (bed 207, 209). These are overlain sulted in an anoxic environment, which in by 14.7 m of pale-dark bedded clays (in turn gave way to finely laminated terval F), which gradually pass into black sediments. Chondrites beds are absent, as clays impoverished in carbonate. is most of the benthos. Belemnites (Aulacoteuthis spp.) are common, rich fi sh Flora and fauna: The Gott pit is one of faunas have been described from these the best studied Lower Cretaceous sections beds (BRAHMS 1913) . The corg content reaches in NW Germany. Micropalaeontologic up to 4%, that of the normal clay facies is groups studied in detail are palynomorphs only 1.8%. Rich assemblages of calcareous 1982; MuTIERLOSE & HAR 1987a, (BELOw oing nannofossils and dinoflagellates have been b; HARDING 1990; LUTAT 1991), calcispheres described from the Hauptblatterton (KEUrr 1980, 1981, 1993), calcareous (MurrERLOSE & HARDING 1987b). The calcare nannofossils (MUTTERLOSE 1991) and ous nannofossils are enriched in foraminifera ( LUTZE 1968; HEINRICH 1991 ). monospecific layers, causing the lamina Macrofaunas include ammonites and tion. These beds have presumably been belemnites (MUTIERLOSE 1983; Figs. caused by a stable water stratification of 41-47). Based on the floral and faunal content six warm surface waters and seasonal palecologic intervals (A-F) have been dif phytoplankton blooms. fe rentiated (Fig. 39). Interval D: Re-establishment of normal Interval A: Clay-marl rhythms of the marine conditions. The floras and faunas Hauterivian. Rich and diverse micro- and are, however, impoverished in comparison macrofauna, representing a well-oxygen to those of interval B. This may have been ated environment. The Boreal ammonite caused by a decrease in oxygen. Boreal and Simbirskites (S. gottschei, S. genus (C.) (C.) endemic floras and faunas are common. discofalca tus, S. (C.) juddii) and the The black clays of the Oxyteuthis depressa Tethyan Crioceratites strombecki occur. belemnite Zone are essentially barren of The belemnites are of Tethyan (H. microflora and fauna. jaculoides) and Boreal provenance (Acro teuthis ra wsoni, A. stolleyi). The dis Interval E: Well-oxygenated shallow-wa tribution of the microfauna and -flora is ter sediments, rich in benthic and plank comparable to that of the Frielingen sec- tonic foraminifera (Hedbergella). The rich ,_.- - .. ·· · - ' I i - ' · · · I - I ,.. ( ;' I " . !• .. 3 41. Heteromorphs from the Late Hauterivian discofalcatus Zone, Gott clay-pit. 1,2. Criocera rires Fig. srrombecki, ventral and lateral view. 3 . Criocera rires srrombecki. Specimens from the collection of K. WIEDENROTfl. All figures are x 0.4. 67 2 ..... - .· .... . ·��·"" . "· �:. . 3 Fig. 4 2. Heteromorphs from the Early Barremian rarocinctum Zone, Gott clay-pit. 1 2. Hoplocrioceras , rarocinctum, ventral and lateral view. 3. Hoplocrioceras cf. rarocinctum. Specimens from the collection of K. WIEDENROTH. All figures are 0.75. X 68 /}�- - �·tt ·<;� t� _ ·� ' ' • .< i_::....� ... ! 1 Fig. 43. 1,2. Hoplocrioceras ra rocinctum, Early Barremian rarocinctum Zone, Gott clay-pit, lateral and \·en tral view. Specimen from the collection of K. WIEDENROTH, x 0.4. and diverse nannofossil assemblages con of the Nolaniceras nolani and sist of abundant Rhagodiscus asper and Hypacanthoplites jacobi ammonite Zones Na nnocon us truttii. This assemblage re has a widespread distribution in NW-Ger fl ects a major warm water pulse of the many (jacobi-nolani Clay). Recently two nutfieldiensis Zone, present throughout the specimens of N. nolani have been found in North Sea. The nannofossils and this interval, confirming the age assign microfauna are associated with ment. Neohibolites inflexus. Elsewhere the same beds yield the Tethyan belemnite Duvalia Pale-dark bedding rhythms: Interval grasiana. A (Late Hauterivian), which is about 12 m thick, is characterized by typical bedding Interval F: This interval is characterized rhythms. These consist of 11 clay-marl by increased water depth and reduced oxy rhythms, each of these rhythms having an genation. The diversity of nannofloras and average thickness of about 0.9 m. Carbon microfaunas decreases, macrofaunas are ate contents vary between 4% (sample 58/ 27% 7311) also impoverished. This black clay facies 2) and (sample in the pale lay- 69 3 4 2 1 5 6 8 9 10 Fig. 44. Barremian heteromorphs, Gott clay-pit. 1. Hoplocrioceras sp., Hauterivian/Barremian boundary interval. 2 . Hoplocrioceras sp., Hauterivian/Barremian boundary interval. 3,4. Parancyloceras bidentatum, ventral and lateral view, bidentatum Zone. 5,6. "Crioceras" sparsicosta, lateral and ventral view, stolleyi Zone. 7 . Pa rancyloceras scalare, bidentatum Zone 8,9. Hoplocrioceras phillipsi, ventral and lateral view, rarocinctum Zone. 1 0. Hoplocrioceras phillipsi, ventral and lateral view, rarocinctum Zone. Specimens from the collection of K. WIEDENROTH. All figures are x 1. 70 1 4 5. Late Barremian heteromorphs from NW-Germany. 1 . Criocera tites sp., denckmanni Zone, Mellendorf Fig. clay-pit. 2. Cri ocera cices sparsicosca. scolleyi Zone, Berenbostel clay-pit. 3. Criocera tites tuba. denckmanni Zone. Mellendorf clay-pit. 4. Criocera tites tuba. denckmanni Zone, Mellendorf clay-pit. Specimens from the collection of Niedersachsisches Landesmuseum, Hannover. All figures are x 0.75. 71 46. Barremian heteromorphs from the Hannover-Aegi section. 1. Criocera tites roeveri, Late Barremian Fig. elegans Zone. 2. Criocera tites aequicostatus. Late Barremian elegans Zone. 3,4. Hoplocrioceras fissicostatum, Early Barremian fissicostatum Zone. Specimens from the collection of K. WJEDENROTH. All figures are x 0.5. 73 Fig. 48. SEI\1 photographs of calcareous nannoplankton from the Blattenon, Barremian NW Germany. The bar in the lower right corner equals 1 micron. 1 . Enrichments of Scapholithus fo ssilis, Late Barremian germanica Zone. Hoheneggelsen clay-pit, bed 118. 2 . Enrichments of Nannoconus abundans, Early Barremian Aulacoteuthis Zone (Biatterton horizon), Gott clay-pit, bed 100. 3. Enrichments of Truncatoscaphus pa uciramosus, Rhombolithion bifurca cum, Lithraphidites carniolensis, Late Barremian germanica Zone, Hoheneggelsen clay pit, bed 118. 4. Manivicella pemmatoidea, Rhombolithion rh ombicum, Vagalapilla matalosa, Late Barremian germanica Zone, Hoheneggelsen clay-pit, bed 118. 5. Enrichments of Lithraphidites carniolensis, Late Barremian germanica Zone ( Blatterton horizon), Hoheneggelsen clay-pit, bed 118. 6 . Lithraphidites carniolensis, Zeugrhabdows spp., Scapholithus fossilis, Late Barremian germanica Zone (Biatterton horizon), Hoheneggelsen clay-pit, bed 118. Enlarged view of Fig. 5. Fig. 4 7 (opposite page). Barremian belemnites of the subfamily Oxyteuthinae from NW-Germany. Each specimen is shown in ventral (left) and lateral view (right). 1,2. Aulacoceuthis compressa, Early Baremian Aulacoteuthis belemnite Zone, Gott clay-pit, bed 100. 3 , 4. Aulacoteuthis compressa, Early Baremian Aulacoteuthis belemnite Zone, Gott clay-pit, bed 100. 5,6. Aulacoteuthis absolutiformis, Early Barremian Aulacoteuthis belemnite Zone. 7, 8. Oxyteuthis brunsvicensis, Early Barremian brunsvicensis belemnite Zone, Gott clay-pit, bed 116. 9, 1 0. Oxyteuthis depressa, Late Barremian depressa belemnite Zone, Westerberg clay pit. 11,12. Oxyteuthis depressa, Late Barremian depressa belemnite Zone, Westerberg clay-pit. All figures are xl. 74 Hoheneggelsen Polder Wl Layer No. 120 I-XVI High Corg-values of both the Blatterton and the Fischschiefer (2 to 6%) support this idea. Carbonate values can be as high as 50% in the Blatterton and in the Fischschiefer. These laminated sediments have been recently studied in quite some detail by the German Apti-Core working group, a special volume of "Cretaceous Re search" is dealing with this topic. Blatterton and Fischschiefer differ by their hydrogen index. The Aptian Fischschiefer contains more marine organic matter than the Barremian Blatterton, while the latter yields IV VI VIII XII XIV XVI +------approx 20 mm ------more terrigenous organic matter (Fig. 50). -e- Otverstty _.._ Rhagod1scus spp. pale layer The spatial and stratigraphic distribution � 81scutum constans -+-- Watznaueria bamesae dark layer of the Barremian and early Aptian lami nated sediments indicate deposition under 49. Nannoplankton associations from a Late restricted conditions in a marginal sea (Fig. Fig. Barremian Blatterton horizon of the Hoheneggelsen 52). The earliest Blatterton occurs in the section. (after ScHAAF, unpublished). basin in the latest Hauterivian. This coin cides with the closure of the Carpathian sea ers, and between 6% (sample 64/3) and way towards the Tethys. This change of the 15% (sample 70/2) in the dark layers. palaeoceanography caused significant In the eastern part of the NW-German Ba changes of the oceanic circulation pattern. sin, clay-marl bedding rhythms have al In the Hauterivian, the NW German Basin ready been observed in the Early had open sea-ways towards the south and Hauterivian (Endemoceras amblygonium north, while the sea-way towards the south ammonite Zone). These bedding rhythms was closed in the Barremian and earliest become most conspicuous in the Aptian. These palaeogeographic conditions Hauterivian/Barremian boundary interval. make it plausible that the laminated They are, however, absent in outcrops situ sediments formed in a marginal sea under ated in the centre of the basin. Sections in stagnant conditions (stagnation model). An the eastern part of the basin show distinct exchange of water masses towards the north Ch on drites beds, which are absent in the was restricted by the Pompeckj Swell, an centre. The nature of these bedding area of non-sedimentation separating the rhythms is discussed in more detail in the NW German Basin from the North Sea area. Frielingen section. Anoxic conditions were caused by a stable water Stratification (MUTIERLOSE & HARDING Laminated Sediments: The Barremian 1987a, b). In the central part of the basin and early Aptian of NW Germany and the in particular, a stable water stratification southern North Sea show distinctive lami caused by warm surface waters prevailed nated sediments (Hauptblatterton, over certain periods. At the same time, Blatterton, Fischschiefer). These consist of waves and storms in the shallow marginal alternating pale and dark laminae. The pale environments permitted the oxygenation of laminae are composed of monospecific the bottom waters, resulting in the deposi enrichments of calcareous nannofossils tion of non-laminated sediments. Seasonal (Fig. 48, 49), the dark laminae are enriched phytoplankton blooms of the warm surface in dinoflagellates. The thickness of a pale water caused mono-specific enrichments, dark lamina varies between 50 and which are preserved as pale laminae. Or 150 llm.The pale laminae are about 60 llm ganic-geochemic studies show that the lami thick, the dark ones about 35 llm. Diver nated sediments have a higher portion of sity and abundance of benthic organisms marine organic matter in comparison to the is extremely impoverished. Good preserva coeval black clays (Fig. 50). tion of nectonic organisms indicates depo The last laminated horizon, the sition under anoxic conditions. Well-pre Fischschiefer of the Early Aptian served fish faunas have been described Deshayesites deshayesi ammonite Zone, from the Blatterton and the Fischschiefer. was clearly deposited after the turnover of 75 thermocline encroached onto the basin margin, causing anoxic conditions here as well. The Late Barremian could, how ever, reflect a slightly cooler phase. Dur ing these periods anoxic conditions pre 750 vailed in the basin, while the basin mar gin was rather well oxygenated. After the c, deposition of the Fischschiefer a major, 0 u large-scale palaeoceanographic change .!?' 600 u occurred. J: Cl Recent finds indicate a water stratifica §. • X tion for the Early Aptian Fischschiefer Q) 450 "0 caused by a fresh-water influx. .E c: Q) Cl !:2 "0 300 >- J: 1 50 0 50 100 1 50 Oxygen Index (mg C02/g Corg) Fig. 50. Hydrogen/Oxygen-index: comparison of various sediments from the Early Cretaceous (after j[t-:lJRZEIE\\"S"I 1995 ). greyvalues of the Hauptbliinerton (Gon) 200 the planktonic and nektonic organisms. of. 'D This indicates that a thermally stable wa 180 ter stratification existed at least until the .. 160 mid-Early Aptian. While floras and faunas :I 'i.. of the surface waters had already changed, .... 140 the deeper pans of the basin were still char !!"' acterized by Barremian anoxic conditions 120 (Fig. 52). The Early Aptian Fischschiefer has 100 a wide geographic distribution within the :E � basin. The Fischschiefer has also been ob 80 served in coastal settings near the Harz 158 160 162 164 166 168 170 Cenllmetru bel-top oftheH8uptblltterton (Eisenkuhle). A water stratification caused by a fresh-water lens has been proposed spectral analysis of the Hauptblilnarton (Gon) for the Aptian Fischschiefer (MuTIERLOSE et 4000 al. in press). It seems most likely that the 3500 deposition of the laminated sediments was 3000 controlled by two factors: The palaeogeographic framework in 2500 • a; Barremian and Early Aptian times re I 2000 8. sulted in a poorly oxygenated 1 500 epicontinental sea, only open to the 1000 north. 500 Warm-arid phases in the Barremian • 0 caused a thermally stable water stratifi 0.02 0,03 0.04 0,05 0.06 0.07 0,08 0,09 cation. The main warm periods were the frequency late Early Barremian (HauptbHi.tterton) 51. Greyvalues (top) and spectral analysis (bot Fig. and the mid-Early Aptian (Fischschiefer). tom) of a sample from the Hauptblatterton (after NEBE During these warm-arid phases the 1994). 76 References: BELOw (1982); BRAHMs (1913); lfARDING ( 1990); HEINRICH ( 1991); KEUPP ( 1980, 1981, 1993); LUTAT (1991); LUTZE (1968); MUTTERLOSE & HARDING (1987a, b); MUTTERLOSE ( 1983, 1984, 1991, 1995); MUTTERLOSE et al. (in press); NEBE (1994). D Pr-.-a L•11c:1 . ... "-1011l•t- Gcni ..:IIOI'I 52. Palaeogeographic map ofthe Early Barremian Fig. 0 of NW Europe (after MurrERLOSE 199 5). basin basin (Rethmar) (Hoheneggelsen) Legend: - FS ----- ,.J;;�� I ,;;,;.;;;;;;�..lilillii; i.:i:ili� ------.,...... ""1 marl 1/ 1! clay I! -= I! � Blatterton I! = I! FS Fischschieler I/ HBI. Hauptblatterton /j I/ I! I! I! /; margin I! 1 (Gott!Sarstedt) 1 I I I! I! FS - - HBt. 53. Comparison of basinal and marginal successions of the Barremian and Early Aptian (after Fig. MurrERLOSE & WIEDENROTH 1995). 77 2.10 HPCF 11 at Misburg (Figs. 54- moment, they comprise a 500 m thick com 56) posite succession, ranging stratigraphically (by G. Ernst, B. Niebuhr & U. Rehfeld) from the higher Lower Cenomanian to the upper Upper Campanian. Three of these Location and grid reference: 25, TK outcrops (HPCF 11, Germania IV, Teutonia 3625 Lehrte, R: 3559120, H: 5806320. The I) will be treated here. abandoned HPCF 11 (former Hannoversche The exposures are located in the Lehrte Portland Cementfabrik AG) quarry lies at West and the Kronsberg synclines, which the eastern margin of Misburg, northof the are, in their marginal parts, flanked by the canal to the cement factory. NNE-SSW trending salt structuresof Lehrte Sarstedt and Benthe, the genesis of which Introduction: The exploitation of marly is intimately linked with inversion tecton limestones by the cement industries near ics and diapirism (Fig. 54) (BALDSCHUHN,fRISCH Hover and Misburg east of Hannover led to & KocKEL 1985 ) . These structures were af the development of numerous limestone fected by intermittent, halokinetic move quarries which now belong to the most ments and periodic phases of uplift, which important exposures of Upper Cretaceous had an important influence on the strata in northwestern Germany. At the sedimentologic and structural history of the ITJMa astrichtian (krma) rill Hauterivian/Barremian (krhlkrb) ampaman ) WealdenNalanginian (krwlkrv) �c� · (krea .. Santonian (krsa) Jurassic (jl. jb, jw) f::)}.(:'J 1:::;:::: : tl c:=JCenoman ianffuronian (krclkrt) Wll:���,��#:�jTriassic (s, m, k) Albian (krl) Zechstein (z) � [:-/}\}'] � Aptian (krp) f&'� Va langinian-Aptian (krv-krp) Fig. 54. Geologic map of the area between the salt structures of Benthe and Lehrte near Hannover (after ERNST 1975). 78 area during Late Cretaceous times. Based a few exposures remain of an Upper Creta on data derived from numerous boreholes, ceous succession, that is highly differenti BETIENSTAEDT & DIETZ ( 1957) carried OUt a ated. In respect of both facies and basin detailed investigation of the Lehrte-Sarstedt dynamics (Fig. 56), the continuity of this salt structure. Already twenty years before succession is interrupted by the above the paper of VAIL et al. ( 1977) gave rise to mentioned stratigraphically and the "era of sequence stratigraphy", these tectonically induced hiatuses. At a major authors could recognize and date as many NE-SW fault extending from the northern as 16 different transgressive surfaces, wall to the middle of the western wall, black stratigraphically ranging from the Middle shales of the Cenomanian/Turonian bound jurassic to the Tertiary, on the fl anks of ary interval are down thrown ( 40 to 50 m) the Lehrte-Sarstedt structure. Recently, the against light limestones of Cenomanian age. sedimentary cycles of the higher Upper The former are overlain by pale, marly Cretaceous in the eastern part of Lower limestones of the Lower and basal Middle Saxony and western Sachsen-Anhalt were Turonian. On the eastern and northeast treated comprehensively by NIEBUHR ( 1995; ern walls, these Turonian limestones are Fig. 55). overlain discordantly by transgressive Up In the excursion-area, several Upper Cre per Santonian marls, which form a taceous transgressions can be demon conspicious dark water saturated interca strated in the quarries of Misburg and lation between the pale coloured Turonian Hover. The most spectacular one is the late limestones below and the Lower Campanian Santonian Marsupites transgression, which limestones above. The Cretaceous strata are is expressed by an abrupt facies change and overlain by a thin, in places discontinuous, a basal lag containing reworked material layer of fills of the Saale glaciation of the earlier Mid-Santonian transgression. (Pleistocene), which, in turn, are covered Due to the good exposures and the abun by late to post-glacial lacustrine muds with dance of fossils, the quarries of Misburg and an intercalation of Laach-type tuffs (DIETZ Hover have attained a certain fameamongst et al. 1958). scientists and amateurs. It is therefore not Because of the exposed Black Shale succes surprising that, over the last decades, a lot sion and the repeated transgressive events of scientific papers were published on the the quarry has been the subject of relatively Cretaceous of Misburg (see references be detailed multidisciplinary investigations low). As several international and numer (for references before 1975 see ERNST 1975 ous national excursions have visited this and ERNST et al. 1983, 1984). The research area in the past, the sections are now well on the Black Shale facies and its correla known to experts not only in Lower Saxony. tion and lateral interfingering with the Furthermore, the multistratigraphic treat proximal RotpHiner swell facies by HILRRECHT ment of the Misburg strata is of fundamen ( 1986, 1988), HILBRECHT & HoEFS ( 1986) and tal importance in respect of HILBRECHT & 0AH�IER ( 1994) is of particular biostratigraphic subdivision of the importance in this context. Campanian. Additionally, the sections can be shown to represent a link between the Cenomanian: Similar to the succession at West- and East-European fauna! provinces. Baddeckenstedt (No. 6), the Lower In that sense, the sections are of great value Cenomanian (higher dixoni Zone) is char for interbasinal correlation and calibration acterized by marl-limestone alternations of of Campanian zonal schemes. which roughly 15 m are exposed. However, thin, bioclastic mar! layers with micro Stratigraphy: The HPCF 11 quarry exposes phacoids show sharply defined basal bed the dixoni Zone of the Lower Cenomanian contacts and intense post-event to the basal conicalpapillosa Zone of the bioturbation and are therefore interpreted Lower Campanian. The upper Middle as allochthonites with possible derivation Turonian, Upper Turonian and the from the south. This feature is unknown Coniacian is represented by a hiatus. from Baddeckenstedt. The limestone beds are bioturbated and are, therefore, clearly General Remarks: The quarry has been autochthonous. The fauna indicates a abandoned for several years and is used depositional area with only a small degree now as a repository for sand. Today, only of subsidence and, at the most, only very 79 R Stages/ Eustatic Cycles in � R Tectonic Activity � Lithofacies � {! ::!! Substages Lower Saxony and and Diapirism i :!! the Subherzynian � � 0 o SheK basins Swells (condensed :!,�.,..., :i �!. j., � < ::!<�.s �-- �---r---4��;,�rT��rr��rr------���+------�------_,or lore deeps sequences) +�---+--� + TA 1.1 UZA- u HS 4.5 L 74 f-----+-----j Peine Tectoevent L... Q) L 03: ...... J .. ,6&: &: ·!! �� c l!li m 'ii> ::r ii "'"' c Wemigerode 1. 0 Tectoevent i ...... c ]::r � .. m C/lQ. CJ) L Fig. 55. Eustasy, sedimentary cycles and tectonic activity in the Late Cretaceous of Lower Saxonyand Sachsen Anhalt (after NIEBUHR 1995 ). gentle palaeoslopes. Of importance for re Middle Cenomanian succession consist of gional correlation with Baddeckenstedt is bioclastic marls and marly limestones with the proof of the Schloenbachialvirga tus two intercalated hardgrounds (HG I, HG 11). Event. Allochthonous sediments such as slumps The lowermost 10 m of the ea. 40 m thick and slides above HG 11 and, to a lesser ex- 80 m Qu. :�=:::-::::::::\:::: lacustnne marls lake crease in abundance and diversity of plank tills of the Saate------gtacoallan- 11���- .le-( 'el� -.,, � tonic foraminifera (see DAHfi.IER & ERNST I ,�--,_� �� :i 1986). 1 c About m below the MCE, an asso marl/hmestone alternations ciation of Schloenbachia and the � "-''V ./'J /"VI"'V.t"V_,, ,... .,_. secondary � foredeep "-' '1"../ I"'V•"- heteromorph ammonite Anisoceras is sig t 31: nificant for an event that might be located ,3 �'-'(��J' "'-"'I"'vrv _- SB transgression in a transgressive systems tract. 150 =i """1· ¥::¥::�:""-':.--� glaucon•ttcpilula marls SB Above the MCE, the succession is charac Y 'V' Y·.Y Upper Santonian transgnonion � · .'\ -dlnoceramu.s�� terized by incipient hardgrounds, ., .!! promary :g � Ill� foredeep lithoclast-bearing debrites and grey marls. SB event � .!! tlyfJioldes herr:ynicus ii£ � tempeslile facoes The latter were interpreted by HILBRECHT carbonate c: ... . ( 1988) as pre-flow muds. The same author _ llytJioides events -E � � � � _ . r.�mP..... "Upper Black Shale belt" described a 30 m sequence of limestones , Corg1-2% ,_� and marly limestones with shear folds that I � basin ooo1, · "Major Black Shale is penetrated by shear planes. This struc belt" facoes CO C: "V�,.,'""--" rv slides and therefore synsedimentary in ori ..!! ±}::� - plenus aed gin, indicating a marginal position within -3c: 11 .. SB regtonal a primary foredeep of a salt structure. •: gc: "poor teclOMIC 0 rnotomagenseZone) limestone" .. qutescence The lower Upper Cenomanian is character ! (naviculare ized by a return to relatively quiescent sedi mentation. The lower part consists of a bioturbated succession of 6 m mart-lime stone alternations with Schloenbachia slope lym ense, followed by 12 m of white, macro facaes fossil depleted, coccolith limestones, known as the "Arme rhotomagense-Schichten" of guera ngeri zonal age. The Pycnodonte Event, usually taken as the Middle/Upper m•gratlon Cenomanian boundary marker in Lower of the pnmary Saxony has not been recognized from the foredeep from N HPCF 11 section. flow limestone marly Cenomanian/Turonian boundary in c:=:J- deDnsblack shale :..:.:..__J marly 11mestone day • htatus terval (ea. 30 m): Renewed interregional rrn harag•ound (HGI hmy marl m Fig. 56. Generalized section of the Upper Creta tectonism caused an increase in relief of ceous of the HPCF 11 quarry (modified after HILBRECHT the depositional area and an intensification 1987). of halokinetic activities. In the foredeep of the salt structure of Lehrte, comparatively tent, above HG I can be attributed to a thick successions of "black shales" with in lowstand regime that is overlain by the au tercalated white limestones accumulated tochthonous and widespread (overlapping) (ERNST et al. 1983, 1984; HILBRECHT & DAHfi.IER prim us Event. The presence of the event is 1994). This so-called "Schwarz-WeiE.e proved by the typical primus fauna (Magas Wechselfolge" (alternation of black and geinitzi, Terebra tulina nodulosa, white beds) shows a tripartite subdivision /n oceramus sch oendorfi, Hemiaster into a "lower black shale belt" with four griepenkerli) and one single find of the in black beds, a middle "major black shale dex-belemnite Actinocamax primus. belt" with the thickest black beds and an The Mid-Cenomanian Event (MCE; HG green "upper black shale belt", in which the black in Fig. 56) can be recognized by a metre beds again become thinner (HILBRECHT & thick hardground-complex characterized DAHMER 1994), indicating the end of the by two omission surfaces containing green black shale period. The amount of Cor in g stained Thalassinoides burrows. This the well laminated marls referred to as hardground-complex represents the black shales, is very low (1 to 3%). In that interbasinal Mid-Cenomanian non-se sense, they do not represent black shales quence (probably a maximumfl ooding sur sensu stricto. However, the content of car face), which is followed by a sudden in- bon particles is high. The usual positive 81 o 13( excursion within the plen us Event has Event. been proved by HILBRECI-IT & HOEFS ( 1986) also As the Turonian strata were slightly tilted in the HPCF 11 section. The lower and up by the Subhercynian inversion tectonism, per unit, in particular, can be correlated as the Upper Santonian transgression cut far as Lengerich in Westphalia (ERNST et al. Turonian strata of different levels (Lower 1 9 84). The origin of the black shale beds is Turonian and lowermost Middle Turonian HILBRECHT (1986), HILBRECHT COntoversial. in at HPCF 11, Middle Turonian to lower Up BACHMANN & MUTTERLOSE ( 1987) and HILBRECHT per Turonian at the more southerly, but & DAHMER ( 1994) interpreted them as completely overgrown HPCF I quarry) with allochthonites. According to ERNST et al. an angular unconformity. (1983) this interpretation cannot be ac cepted on account of the good correlation Upper Santonian: The Upper Santonian of even the thinner beds between eastern transgression is marked by a weakly devel Lower Saxony and western Westphalia. oped basal horizon of glauconitic marls While the intercalated limestones are very with sparse pebbles. Most of the pebbles poor in fossils, the black shales contain a are edge-rounded, green intraclasts of lime remarkable fauna of mostly large stones derived from the underlying inoceramids. One horizon, the so-called Turonian Planer limestones. Of very spo juddii Event, has yielded crushed pyritized radic occurrence are dark phosphorite peb ammonites, including Neocardioceras bles, originating from the rocks flanking the juddii, Th omelites sp., Worthoceras sp. and salt structure of Lehrte. The transgression abundant Sciponoceras. Furthermore, rem is inferred to have proceeded in a in NW 1968; 1975; NIEBUHR nants of fishes occur in several black shale direction (AL-ABAWI ERNST layers (KRIWET & GLOY 1995) as well as a sin 1995 ) . The completely homogeneous gle find of a swimming crab. Santonian marls are only some few metres thick. Several bedding joints correlate with Higher Lower and basal Middle breaks in the evolution curve of Turonian: The last black shale couplet Gonioteuthis sp., indicating repeated hia (Doppellage) coincides with the lowermost tuses within that sequence (ERNST 197 5 ). and original Mytiloides Event (sensu ERNST The marls yield an abundant and diverse et al. 1983 ), which represents a mass-oc fauna. So far, 13 species of bivalves, 11 spe currence of mytiloid inoceramids in com cies of echinoids, 5 species of brachiopods, paratively shallow water environment. It 5 species of belemnites, 3 species of gas can be traced from the sandstone facies of tropods as well as several species of sponges Saxony and the Rotplaner platform facies were recorded by ERNST (197 5). into the basinal black shale facies of the Biostratigraphic subdivision is based on the excursion area. Good correlation and abun crinoid Marsupites and about 300 speci dant fauna indicate an increasingly equili mens of the Gonioceuthis-lineage collected brated relief and the recovery of water cir bed by bed. culation. As the distribution of the event is Of palaeogeographic importance are the not delimited by facies, it is a classical ex finds of corroded foraminifera and re ample of an overlapping and isochronous worked Gonioteuthis of Mid-Santonian age event, the lateral distribution of which in the transgressive lag, because they ranges presumably from Khazakstan to clearly prove the Mid-Santonian transgres Mexico. sion extending as far as the Misburg area. Ro ughly 10 m above the first Mytiloides This Mid-Santonian transgression can be Event, the Mytiloides hercyn icus Event is correlated over a distance of more than 50 developed within a sequence of light, marly km into the eastern parts of the basin near limestones. In terms of sequence Peine and Meine (NIEBUHR 1995). stratigraphy, it probably corresponds to a floodingsurface. As most of the Rotplaner Lower Campanian: Separated by a hia sections represent shallow water environ tus comprising most of the ment on a swell, the hercyn icus Event is granulataquadra ta and at least parts of the missing there. Only in the southeastern lingual quadra ta Zones, the continous se corner of the quarry, basal Middle Turonian quence starts with a transgressive strata with /. apicalis, I. cuvierii and /. glauconite horizon, concordantly cutting lamarcki are exposed above the hercynicus into the underlying marls. This horizon is 82 References: Asu-MAARUF AL-ABAWI characterized by the abundance of (1975); belemnites and can also be correlated over BALDSCHUHN BETTENSTAEDT (1968); et al (1985); a distance of more than into the east & DIETZ DAHMER & ERNST DIETZ 50 km (1957); (1986); ern parts of the basin (ERNST et ERNST ERNST 1963, 1968; al. (1958); (1975, 1963, 1968); ABU-MAARUF NIEBUHR With the et al. HILBRECHT & DAHMER 1975; 1995). (198 3 , 1984 ); onset of transgression, a long period of HILBRECHT & HOEFS HILBRECHT (1994); (1986); uniform and continuous sedimentation re KRIWET & GLOY (1986, 1988); (1995); sulted in the deposition of mart-limestone BACHMANN & MUTTERLOSE NIEBUHR (19 87); alternations, seen in the Germania IV and VAIL (1995); et al. (1977). Teutonia I quarries described below. 83 Germania IV quarry at Misburg 2. 11 ern wall of the Germania IV quarry. The (Figs. 57-60) succession can be subdivided into at least (by G. Ernst, B. Niebuhr & U. Rehfeld) eight lithologic units (Unit 1-8), mostly separated by distinct marl layers or marl Location and grid reference: TK 25, couplets. 3625 Lehrte, R: 3559900, H: 5804250. The The section starts with nodular, marly lime large Germania IV quarry (now called stones with unconspicuous intercalated, Teutonia 11) lies east of Anderten, south of less calcareous marl layers of Unit 1. The the railway track. top of the unit is marked by resedimentation phenomena, pebbly Stratigraphy: conica/papillosa to intraclasts of calcareous marls, accumula stobaeil basiplana Zones of the "Middle" tions of Baculites fragments, irregular Campanian (uppermostLower to lowermost echinoids ( Galeola papillosa) and sponges. Upper Campanian). The unit is separated by a distinct dark marl layer, poor in carbonate. General remarks: The quarries I to Ill of The following sedimentary Unit 2 comprises the former "Zementfabrik Germania" were a quite well and thick-bedded alternation abandoned about 40 years ago and are now between marlier and more calcareous lime backfilled. At Germania IV, a quarry only stones, relatively poor in biogenic compo slightly affected by tectonism, exploitation nents. This unit grades, without a distinct has been recently resumed at the western top layer, into the following unit. quarry wall. The newly exposed section The interval of Unit 3 comprises thinly bed comprises the fossiliferous higher parts of ded, nodular marl-limestone alternations, the Lower Campanian (conica/papillosa richer in biogenes than the subjacent unit. Zone). The exposed section of Germania IV One horizon, ea. 1 m below a distinctly is 140 m thick and was documented by developed top marl layer, bears a rich KHOSROVSHAHIAN ( 197 2). He investigated the faunal assemblage of Galeola papillosa. section by means of multistratigraphic Unit 4 is characterized by two less marly methods and correlated it with the nearby limestone horizons, each topped by incipi exposed section of Teutonia I. ABu-MAARUF ent hardgrounds and a superjacent, dis ( 197 5) presented detailed micro tinct, dark marl layer. The lower limestone palaeontologic results. By means of a highly horizon has been chosen as a "marker ho diverse foraminiferal assemblage, he devel rizon" in the quarry, since the relatively oped a high resolution ecostratigraphic high carbonate content allows rapid rec framework. The stratigraphic ranges were ognition within the otherwise quite mo proved in the section at the Nordcement notonous succession of more or less well (Alemannia) quarry at Hover, some 3 km developed marl-limestone alternations. from Germania IV. Unit 5 is a couplet of nodular, marly lime stones, separated by a more calcareous Tectonic setting: The Germania IV horizon. The base of the second nodular, quarry exhibits only faint tectonic stress marly limestone bed is characterized by with simple tension faults and occurrences of the echinoid taxa Micraster displacements of less than 5 m. The faults schroederi and Cardiotaxis lehmanni. This show a steep easterly dip which may be unit is topped by a distinct limestone bed explained by an easterly migration of the which can be easily correlated with the fo redeep of the Lehrte-Sarstedt salt struc southern wall of the quarry, where the sec ture. This is substantiated by the develop tion, slightly displaced by tension faulting ment of syn-sedimentary phacoid-like (see above), continues with the folowing shear bodies resulting in small-scale slump unit. and slide structures in the "Middle" Unit 6 comprises nodular, marly limestones Campanian marly limestones and calcare with 2 to 3 weakly developed intercalations ous marls. of marlier beds. It is topped by a more dis tinct calcareous bed which grades into unit Lithostratigraphy and facies: The ea. 7. 2 5 m thick conical papillosa/ gra cilis Zone Unit 7 is a nodular, marly limestone which comprises a succession of calcareous marls lacks any recognizable differentiation. It is and marly limestones, exposed at the west- topped by a distinct, darker marl pair, with 84 ••••••••••••• lmJ .;..·d 1- -=--=' K43b MK7S 1JS KM74 65 ..= �---( =-i MK74 -- K4Jo --.--- �---: KM73 KM4l . - .. .. ( KM72 - MK41 I'"' 130 � -=-i MK72 oo Z - - �---< .IIM..Z.l <( ,g -·- ...... !: K40 z ·c: ��MK71 <(�b�""'!' ��it:5� KM70 MKJ9 f\1'"1 O.. 'i; _ li:o ;l_ tJiioE:J' �C.:�79 ··i:c.--.------st ratum ot fht' !lll typ� .popu lation·- _J Kl9S _ 6 , ss ::E Ill a Q I!I!IU ol Brlrmn,lrllo <( '0 KJ u:S 4 55 m mucrOrtOIO mutronaro �==�--- - KMJ6 _ _ , �·.,.. 1 --- - MK&B • 0:: ::: z -- KM67 UJ� KJS ...... f-- ...______120 <( -=- O.. " I----: KMJ4 �;; I 90 Echmo corts subglubtuo 0 Echmotorys •• con1co A gr. Golrolo poplfiOSO popilloso or a Goltolo pop11/oso bos1plrmo ss m•crosampl t X 80 10 " �;:::::::::;:/ � MK 7 - " �� .. MK 6 K46 0 ) K Sb t-�=� KM4S r.=-��-=1 MKS � �- --= ...;;. --�cK 4b 75 �--=KM44c .. ---=- c - MK 3 �---: KM44t 0 """':50,;;K::li" 57. Detailed stratigraphy of the Campanian of the Germania IV quarry (after KHosRovscHAHIAN 1972). Fig. an intercalated marly limestone bed. more distinct limestone bed. This unit is The topmost Unit 8 of the conica/papillosa/ likewise topped by a distinct marl pair. gra cilis Zone succession, like the underly Above this unit a completely undifferenti ing one, consists of undifferentiated nodu ated sedimentary succession of nodular, lar marly limestones with one intercalated marly limestones starts, which, near the 85 58. Sketch of the Germania IV quarry (after KHosRovscHAHIAN 1972). Fig. base, contains the first Belemnitella lishment of a local ecostratigraphic frame mucronata, indicating the gra cilis/ work. They allow a high resolution calibra mucronata Zone. tion at least within the exposures of the Lehrte West Syncline. For example, Galeola Biostratigraphy: The basic framework of papillosa tends to be enriched at the base the N-German subdivision of the Upper of the marly limestone beds (e.g. KM 2 and Campanian has been developed in the KM 3 in Fig. 57). Ech inocorys conica like Schreibkreide facies of the so-called stand wise develops two significant eco-maxima, ard section of Ui.gerdorf (ERNST 1963; ERNST the first one in the lower conical papillosa et al. 1996; ScHuLz et al. 1984 ). On account Zone (around MK7), and a second one in of their richness in fossils, the cement quar the higher gra cilis/ mucronaca Zone ries in the Hannover area served as ideal (around KM 24). u- AARU (1975) docu As M F exposures to test the validity of the zonal mented species and individual frequency scheme and provided the impetus to ex tend and complete it (KHOSROVSCHAHIAN 1972; graat1s/ mucronsta ARli-MAARliF 1975). zone The zonal scheme is based mainly on belemnites of the Gonioceuthis and __f'WI ....., __ .... _ Belemnicella lineages, irregular echinoids of the Offa scerl Galeola lineages, as well as on the groups of Ech inocorys, Micrascer and Galerices. lnoceramids and ammonites serve as supplementary elements (ScHMID & ERr--;sT 1975; NIEBUHR 1995, 1996a). In gen eral, two index fossils have been used to name each zone. The conical papillosa Zone (also termed conical gra cilis Zone), is char acterized by the index echinoids .--..•� arn::ar ID ...,__ .., ....,__ Echinocorys conica and Galeola papillosa � ....,�__.IlD respectively, and the index belemnite Gonioceuthis quadra ca gra cilis. This zone is superceded by the uppermost zone of the Lower Campanian (according to German authors), which has been termed the gra § r-=-=-=-=-----1 � cilis/mucronaca Zone on the basis of the ==:.a�-: f (') .,....., ...... __ eo-occurrence of the index belemnites 5- Gonioteuthis quadra ca gra cilis and § =.. --=--' � Belemnitella mucronata in this transitional I overlap zone. It represents a well traceable --- marker horizon in the N German Creta --- ceous. - Eco- and event stratigraphy: Apart 0 -1 from sponge-rich incipient hardgrounds 59. Lithology and event beds of the conical Fig. (Fig. 58) echinoids are best for the estab- papillosa/ gracilis Zone in the Germania IV quarry. 86 marly hmestone ci mar1.tcne "' rnar1 - prominent mar! layer 'V ·- bed (opoka) y glauconitebedded � ��:�: ::: -ed � -� & "t:: 1------� o::� � Standard !: � � e sectionof � :: ...: � ltleLehrte Mallrobiazonationwith 1! � WestSyncline. 1; 1; A=ALEMANNIA echinoids, belemnitiM o.Qi"'Qi quany, T=TEUTONIA and ammonites <.!l <.!l <.!l quarry. m Exitelocell!ls bipunctatum I + Galeritas + roemeri Csrdiasler 500 ' c: corriiformis I'll + "E Belemnitells Ill a. minor E ..., 0... CD a. a. T: 1751 177 :::;) T: 173 mmorlp oly T: H11 1n 400 CD plocumzone T: 152 .!! T: 1481 1<491 ISO "' I T: 1431 144 "' T: "' 1371140 13&'139 "' "' T: 0 T: 133 "vulgaris"/ "' 1281 129 slo//eyizone 1241 125 1201 121 "' 0 0 0 300 "' T: 104 c: ..., "vulgens "/ � "E basiplenezone ..., 94195 a. T: 92 E ..., 0 CD... T:.1101 61 . a. stobeailbasi 58159 Q, planazone 200 � T: 415 >. T: 39 1:..., T: 33 CD T: 28129 i I . 22 comes/mucro- nsta zone T: 101 111 12 T: 7 atezone � A: 148/ 150 Cl l "' "' .._c: A: 140 100 CDC'IJ "' A: 1181122 conics/ i 3: "E pepi//osazone "' A: 1081 112 ocv ...,1 0. A: 85 CD E 0 73 I "' e"' A:81 _ ..., Ac "' A: 41143 .!! u ! '�' � I '"'' A: 25127 40 !c � A 7 :3151 "ula • lii!liiililiii! >. . lingua/que- 20 1:"' ... � dlllllazone CD ...I i" 0 i 60. Range and abundance of irregular echinoids from the Campanian of the Lehrte West Syncline (Hover Fig. p:::::cl���=:::::J�� ���II Misburg-Ahlten area; after ERNST 1975 ). � curves of foraminifera, their acme-occur inter-quarry correlations. rences and plankton/benthos ratios as well as frequencies of agglutinating and calcar Facies pattern and biostratonomy: eous taxa for ecostratigraphic and facies The typical benthonic faunal assemblage analyses. The individual frequency curves of the marly limestones of the Misburg area proved to be the most suitable method for is characterized by siliceous sponges with 87 a rigid skeleton ("lithistid" demosponges boundary between the conicalpapillosa and hexactinellids) and irregular echinoids. and gra cilis/ mucrona ea Zones. The Both groups exhibit distinct differences in Subhercynian was uplifted, the remote frequencies and morphotype variabilities, northern parts, e.g. the Beienroder Basin, despite the relatively monotonous carbon the Allertal Graben, etc. were flooded ate facies of the section. Siliceous sponges (NIEBUHR & ERNST 1991; NJEBUHR 1995). With mostly settled on hard substrata of the in the so-called mucronaea transgression, cipient hardgrounds during times of very closely above the uppermost marl couplet low sedimentation rates, where they formed of the conica/papillosa Zone (Fig. 59), cluster-like accumulations. In the case of Belemnieella mucronaea migrated into the the echinoids, Echinocorys conica occurs area from the Russian platform. Contem preferentially in the carbonate richer, poraneously, or slightly later in the gra ci Galeola papillosa in the marlier lithologies, Jislmucronaea Zone, short-termed invasions so that in some of the typical marl-lime of Belemnellocamax mammilla eus, stone pairs, the former succeeds the latter. Boserych oceras (Mobergoceras) indicum, Even the nectonic fauna like Gonioeeuehis Pa eagiosites stobaei and certain exotic exhibits some degree of facies depency. spatangoids, probably from the While G. quadra ea quadra ea still dominates Scandinavian coast, took place. in the marlier beds, the guards in lime Another immigration episode, connected stones already exhibit the typical charac with the so-called spiniger transgression, ters of the slender G. quadra ea gra cilis. is documented at the boundary between the Slight differences in the lithofacies influ conical m ucrona ea and stobaeil basiplana ence the size and morphology of some Zones. Paeagiosiees scobaei reappears, now echinoids. A good example is provided by significantly more abundant and with the diverse morphological variations in the larger forms than in the lower occurrence. Ech inocorys conica group, which are clearly Tra chyscaphiees spiniger extended its area not related to phylogenetic development of distribution and rare occurrences of (as COnSidered by KHOSROVSC:HAHIAN 1972) but Belemnellocamax balsvikensis has been re seem rather to be facies-dependent. corded (CHRISTENSEN & ScHULZ 1976). The ex According to the measurements of act stratigraphic position of the southern KHOSRO\'SC:HAHIAN ( 1972), belemnite rostra at immigrants, such as the rare rudistid bi some horizons display preferred orienta valve Agriopleura suecica, within the Lower tion, indicating temporary hardening of the and Upper Campanian, has not yet been seafloor, with currents towards the south determined. The dominating echinoids, east. belemnites, etc. display distinct affinities with the boreal Chalk on the one hand and Faunal migrations and palaeobiogeo with the southeasterly temperate province graphy: Apart from some minor eustatic (Caucasus, etc.) on the other. Connections sea level oscillations, the Germania IV sec with the Westphalian marginal sea, were tion displays two distinct transgressive clearly less good, Echinocorys conica for pulses which correlate with the appearance example is rare and immigrated only dur of new organisms. Both events are related ing a short period. to an only weakly differentiated "bedded calcareous marl facies" (sensu NIEBUHR References: ABu-MAARUF ( 197 5 ); CHRISTENSEN 1995 ), which is underlain and superceded & ScHuLz (1976); ERNST (1963); ERNST et al. by marl-limestone alternations and prob (1996); KHOSROVSCHAHIAN (1972); NIEBUHR & ably reflect temporary shallowing (see Fig. ERNST (1991 ); NIEBUHR (1995, 1996); RIEDEL 57). (194 2); ScHMID & ERNST (19 7 5); ScHULZ et al. In the course of the "Peine Phase" (RIEDEL (1984). 1942 ), inversion tectonics initiated at the 89 2.12. Teutonia I quarry at Misburg 48 and 7 3%, sharp contacts between marl (Figs. 61-64) and limestone beds are not developed. The (by G. Ernst, B. Niebuhr & U. Rehfeld) section can be subdivided into three lithologic units, comprising the upper "vul Location and grid reference: TK 25, garis" I stolleyi and the lower minor/ 3635 Lehrte, R 35 60300, H 58 05300. polyplocum Zones. North of the railway track between the east Unit 1 (cycles 1-8 in Fig. 62) consists of side of Misburg and Autobahn A 7. eight marl-limestone cycles generally com posed of limestones with 5 to 7 intercalated Stratigraphy: Upper conicalpapillosa marl layers in three cases, respectively. Zone of the Lower Campanian to the lower Each cycle starts with weakly developed part of the minor/ polyplocum Zone of the marl-limestone alternations and ends with Upper Campanian. No significant hiatuses a distinct marl couplet, which provides a have been identified. The Lower Campanian conspicuous contrast with the sub- and section is poorly exposed in this quarry. superjacent limestone beds. The higher Only the stratigraphically younger por limestone beds within a cycle, especially in tions, exposed in the southeastern corner cycles 2 to 4, or the base just above the last of the quarry, comprising the transitional cycle (cycle 7), contain calcareous nodular successions between lower and upper Up concretions; these represent the calcified per Campanian ("vulgaris" I stolleyi and tissues of siliceous demosponges with minorlpolyplocum Zones), will be referred monaxone spicules ("soft sponges"). Sponge to in this guide. fragments and foraminifera may also be associated with the sponge bodies. Several General remarks: The Teutonia I quarry of the spicules within these concretions are is one of the largest cement quarries of the preserved as silica, but most of them be Lehrte West Syncline. A total thickness of came calcified. In exchange, the dissociated 260 m of sediment is exposed. The quarry silica replaced most of the foraminiferal exhibits only minor normal faulting. For tests within the sponge concretions. Many several years exploitation has been re of the nodules exhibit an internal septarian stricted to the eastern quarry wall, whereas texture, implying a pore-filling origin particularly the western and northern walls NGELH DT (sensu E AR 1973). These nodules may are very degraded and barely accessible. indicate reduced accumulation rates dur The bedding planes in the lower parts of ing their formation (see MOLLER & FABRICIUS the section dip at zoo to the ESE towards 197 4 ). Bioturbation of the marl layers of the centre of the Lehrte salt structure unit 1 is largely limited to a Ch ondri tes foredeep. The dip decreases to 12o towards ichnofauna, whereas other trace fossils are the quarry wall exposing the upper portion common in the limestone beds. of the section. The superjacent unit 2 (cycle 9 in Fig. 62) The Lower Campanian and lower Upper is characterized by a distinct facies turno Campanian has been studied in detail by ver, which reflects the first regressive KHOSROVSCHAHIAN (1972), WhO measured the trends of the polyplocum regression with section and investigated the faunal content. onset of lowering of the sea level. This unit The deepest parts of the section correspond is a "bedded calcareous marl facies" (NIEBUHR stratigraphically to the Germania IV quarry 1995) and only weakly differentiated by described above and therefore do not need marl-limestone alternations, implying that further explanation. In the highest portions the carbonate content of 60 to 70% remains of the exposed section, the gradual transi rather constant. Only beds h and j are de tion from the so-called "Misburg facies" veloped more distinctly. The former con with marl-limestone alternations to the tains a basal Fe-rich sponge layer, the lat "Opoka" facies of Ahlten is seen, first stud ter is a prominent limestone bed. ied by NIEBUHR (1995). Unit 3 (cycles 10-11 in Fig. 62), which is characterized by marl-limestone alterna Lithology: The newly investigated high tions like unit 1, indicates that deeper wa est part of the section is about 70 m thick. ter conditions prevailed once more before It is characterized by marl-limestone alter the ea. 140 m thick shallow water "Opoka" nations which alternate on a decimetre facies of Ahlten developed, which is no scale. The carbonate content varies between more exposed in the Teutonia I quarry. 90 =···· .. �--- .:...::, . 1.11 ••7: l �:� MIU�F::: f ��: .. 1 " IMJI · '"' 1.11 " i1\:1·� .. .. ...... !!!Ill IUI•Illlll.lrftl 1111 ...... ... ,. ...,. ...,••••••• lllll' ,_,, .. ,. D••· .. . .. .. ••u '" llll,l.f.,fiKIIIoiUI E3 ...... , ...,111111 E3 ... Mol IIIIIDFIIC.CIItfl �!!!!!! ...... ll•t•••ll lll ...... � o .. . . u.,. MOCPII Ilurr.fl.. ...nl E3 ICI•ocMtt•ll ll llhllt m ... 1.11 ... .. ll.llllllol&r .... '" '·' a tu•- ••t. ,' ..·''''''.... IUUO 0 .,,.,lll ...llfloCIII Lifln " 10 H?OIGta 'llo .. ...::::�::;:< �.ii�l,.;:_ �!�.'O •o to 10 to• CeCOJ 61. Biostratigraphy, lihostratigraphy, and carbonate contents of the Teutonia I quarry section (after Fig. KHOSROYSCHAHIAN 1972). As canbe seen with the SEM, the sediments ble. This suggests migration of the carbon of the entire section exhibit pervasivecal ate solutions within the system, probably cite neomorphism, resulting in strong dis from the primarily carbonate-poorer into solution of the calcareous nannoplankton, the carbonate-richer beds of the alterna which consequently becomes undetermina- tions (NIEBUHR 1995 ). The marl-limestone 91 <178l .. (bed numbers partly after 1 1 1972) KHOSROVSCHAHIAN (175)m�: J (174) (173) Nostoceras (B ) polyplocum polyplocum 10 J (1 72) BelemniteUa. Echinocorys pyramidalis. Galerites roemeri. :::> :=;::::t7··. · 1: (171) Neoltothyrina. Cretirhynch1a an::uata. Cameothyris camea. ""- }Plag/ostoma. Pseudo/mea Ill Gl q u §8§ >- _ u ) Nostoceras (Bostrychoceras) po/yplocumpo/yplocum, :"":' p , ' Nostocems (B) polyplocum secoense. ':" 0 " cf. c;::::lP�. n Je/etzkytes compressus. Hoploscapllites greenlandicus juv. _ . m 9) - . k - I ...: .. �:�.ll.· ...-,·.!.�� 8-=8)'G'..._-:rf Nostoceras {Bostrychoceras) polyplocum unituben::u/atum. i Jeletzkytes compressus. Hop/oscaphites greenland1cus. c Trachyscapllites pulcherrimus, Trachyscapllites sp�mgerposterior 1111 c @�d 1111 Cl. 8-=8 } E -�.;. ) c 1111 a b 0 - ) (152) -Gl 1111 ) (151) ..J 8 (150) -Gl (1-49) .!! Nostoceras (Bostrychoceras) polyplocum polyplocum, -=L:J Y')) (148) Baculites, Galerites "vulgaris". Be/emnitella, Ba/hrotomana Gi c: (147) 0 7 N ) (146) M1craster (lsomicraster) stolleyi, Baculiles. Gaterites "vulgaris ". Belemnite/la � -=u � (1-45) :!g <=<=<=)(14-4) � 50 70 80 � (143) 60 • ·� (142) ea 6 ? � ) (141) (140) Pachydiscus haldems1s ? - (139) cl Belemnitalla woodii c (138) Belemnitella 1111 woodii c (137) ea (136) Cl. 5 E � (135) 1111 0 (13-4) -Gl 1111 ===.> ..J (133) >- (132) -.::: 4 50 60 70 80 1111 (131) Ughtness Gl �� ) ) (130) D marly limestone =<=<;;;:>� Pachydiscus haldemsis imy marlstone (129) cf. D = weak marl layer JJJp (128) Trachyscaphiles spinigerspmiger 3 !§I .. (127) marl layer Gl . . . - c prominentmarl layer 0 - N nodular ... (125) c:::> Gl 2 . ---- -· - � (124) platy .5 (123) M1craster (lsorrncraster) stol/ey1, €> ammorite bed Q. t:l: Parasmil1a centralis event bed Ill ..... e; fossil 2m 1 sponge bed � V Fig. 62. Upper Campanian biostratigraphy, lithology and cyclic stratigraphy of the southern wall of the Teutonia I quarry. alternations are foraminifera calcisphere Fauna: The faunal assemblages of the sec wackestones. In the higher part of the sec tion vary parallel to the lithological devel tion (unit 2), the matrix yields increasing opment. concentrations of monaxone, siliceous Unit 1 (cycles 1-3) is rich in biogenic com spicules. ponents like pycnodonteine oysters, some 92 more, the fauna comprises cidarid echinoids, large brachiopods ( Cretirhynchia norvicensis, C. arcuata, Neoliothyrina obesa, Carneithyris carnea, Terebra tulina chrysalis, Kingena pentangulata, Magnithyris magna) and a highly diverse bivalve fauna. The pectinid bivalves (Mimachlamys cretosa, M. mantelliana, Chlamys undulata, Syncyclonema membranaceum, Neithea quinquecostea), pycnodontid oysters (Pycnodonte vesicularis, Hyotyssa semiplana), Spondyl us dutempleanus and Inoceramus haldemensis are abundant and already relatively large. The sponge fauna is characterized by rhizomorine taxa like 63. Sketch map of the southeastern corner of Fig. Seliscothon sp .. The entire faunal associa the Teutonia I quarry. tion is likewise characteristic of shallower water environments. For more details of corals (Desmophyllum sp.), echinoids such macrofossil occurence in unit 2 see NIEBUHR as Galeri tes "vulgaris" and Micraster ( 1995, 1996a). (lsomicraster) stolleyi, rare ammonites Unit 3 is poor in fossils. ( Tra chyscaphites spiniger) , belemnites (Belemnitella sp.) and sponges. According Sedimentation pattern and cyclicity: to ULBRICH ( 197 4) the sponge fauna, contain The mart-limestone alternations are inter ing corallistid demosponges such as preted as climatically controlled cycles, Pa chinion scriptum, indicates shallower reflecting orbital forcing of the water conditions. In the superjacent beds Milankovitch frequency band (MILANKOVITCH sponges remain diverse but contrary to the 1941 ). Sedimentary anomalies like lower portions, taxa like the tetracladinid, tempestites and turbidites are largely miss thick-walled Phymatella sp., pachastrellid ing (NIEBUHR 1995). NIEBUHR (1995, 1996B) taxa like Propachastrella sp. and and NIEBUHR & PROKOPH (in press) have lychniscosan sponges (Becksia sp.) now proved, that the 50 m cycles in boreholes suggest deeper water conditions. The up of the deeper Upper Campanian (conical permost limestone bed of cycle 7 yields a senior to vulgaris! basiplana Zones after more diverse fauna, rich in baculitids, KHOSROVSCHAHIAN 1972; see Fig. 61) can be echinoids, belemnites, gastropods, assigned to the long eccentricity of 400.000 Dentalium sp .. One fragment of Nostoceras years and that the 12.5 m cycles reflect the (Bostrych ocers) polyplocum from the col short eccentricity of 100.000 years. The lection Of KHOSROVSCHAHIAN may well be as boreholes in the deepest parts of the Lehrte signed to this event bed, and indicates the West Syncline show sediment accumulation boundary of the lower/upper Upper rates of 125 m/ma, consequently. The same Campanian in Fig. 62. long eccentricity cycles in the Teutonia I The bedded calcareous marl facies of unit quarry, in the marginal parts of the 2 exhibits a completely different faunal foredeep, have a sediment thickness of 27 spectrum. In addition to faunal elements to 28 m and show accumulation rates of of the subjacent unit 1 like Galerites "vul 68 to 69 m/ma. garis " and some rare M. (lsomicraster) sp., The cycles of unit 1 of the "vulgaris" I it comprises a fauna which is already stolleyi Zone with their bundles of 5 to 7 reminescent of the shallow marine "Opoka" couplets have a sediment thickness of about facies of Ahlten (NIEBUHR 1995; NIEBUHR et al. 5 to 7.70 m (Fig. 62). The carbonate con in press). Scaphitid ammonites, like tent of 48 to 7 3% shows a decrease of bio ]eletzkytes compressus, Hoploscaphites genic carbonate productivity. The subja greenlandicus and T. pulcherrim us come cent mart-limestone alternations of the in (NIEBUHR 1996a). The baculitid ammonites conicalsenior to vulgaris/ basiplana Zones, are significantly broader than in the sub on the contrary, show a relatively high car jacent rhythmically bedded unit 1. Further- bonate content of about 65 to 90%. 93 0 ...,.,.ad(in 1-) c:::::::J morty- .. ., I2SZJ - -��-@ c: rv ...., ..! ., en ·� I .. ::] iJ c E!' - ---· ·.,a� <>...E ·- .!! I -� .. V' -bed("'"*") .... 'b ...... E e E y gill- ....., .. :s't: . :9oe· c: - � � ::] ,,..a ---· -� - - .c: r: � ., .. § - connedlld Q. .5; -�� : I) -....; ., u �-- indlllll'ld �-� �UCCWo�Nel��� �"' l; owlubonory �·- Ill e .., :.t-:.t-aef"U .c: � !! § -2 c�nrtel • Qj .. Cl .2 � c "' 'ti:�� .s. 0 �S"3l:=:: � �p. �!:'.. .Q .Q t:oStwldanl r- ... -�� g:::: � c: c: .i!_ Q...... "' .c: a.uQ.Q. .c:.c: "' :::0 u u ., ., HCtion of ., "' u I! Jl .!! ..!! .. I! I! the Lehrtlt � �� �� -� .!.! u .... MllkrlllliozDnnon with .c �=����� �f"'., "' , g. g. uu WestSynoline, .c:.c: �� � !:: -2 .2.!=!A=ALEMANNIA t Q.Q.Q. .. .,., echinoidli, blllemnilllli � -2-2 )!! u :t::t:g. g. "" quarry, " :t::t:g.g. ati:-£-£ T=TEUTONIA and.mmonilllli Cl) (l)(l)(l):nnl t-::!!....: .:.,;:� ,f � quarry. Exitelooeras - + bipunctstumGelerites + � TD817'HiriCarrbester �0 �Cl N 500 corrliformis + Belemnite/le ·cCl Q. minor ClE c::J 0 c::J I c::JCl �.... c::J L) cc::J Q. c::J Q. T::1 17.l75/ ln t c::J :;) 1111 1n � minor/poly- c::J r • c::J 400 - c::J plocum zone c::J .!! c:::::� c::J r-- c::J T. 14811491150 c::J � � T: 152 c::JCl [§ Cl �T I43/I..C ? ? c::J �. l�/1381139 = c::J � c::J T: 133 c::J "vulgaris "/ c c::J T: 1:zat 128 zone c::J T: 1241 125 c::J sto/leyi �gs� T: 12!1/121 c::J c::J c::J - c 300 c::J T: 104 � c::J "' c::J c c::J T: � basiplana"\lu/garis"l zone "' Cl 94195 c T: 112 Q. ""' cCl E Cl) Cl � Cl Cl C'l c c Cl .5 Cl 0 c 61Y61 �... Cl c::J T: � c 58/59 a. stobeeilbaSI- c T: a. plans zone 200 :;) >. 0 0 T 48 � 0 Cl 0 Cl T. 39 "' c::J � ICl I "" Cl 0 "" T21!1T 3329 ·I 0 Cl Cl Cl T22 conica/mucro Cl nata Cl zone � &! 101 11112 .Q Cl T nata zone T. 7 1---t��;ro.--i :5! 1481 150 100 � 0 A � .!! conical 140 31: � zone 11811221081 112 papi/losa A. ...Jo a Cl)01� "' f------! 'Q. .! zone e 85 papillosa g A.A:61 7.l !i ;zone .!! 0 (.) :5 40 0 Cl A 41143 nensis zone Q. g A25127 · zone A. J/517 >. p1lu/a .9- :5Cl 20 -� � "' t-=lingualqua-:::.::.;===-----1 .c; g � � d � z ""'� � ·.-':V o�--...J--�-�_ __�----�--�:5�------�----�---L�----�rV----��:{"�--�--' --h------�'I"V Fig. 64. Range of ammonites of biostratigraphic significance from the Campanian of the Lehrte West Syncline (Ht:iver-Misburg-Ahlten area; after ScHMID & ERNST 1975; ERNST 1975; NIEBUHR 1995, 1996). Geochemic data (REHFELD et al. in press) in obvious in the K/ AI and associated Si! AI dicate that the cycles 5 to 7 exhibit regular and Ba/Al ratios. This is referred to shifts shifts of the detrital phase at a 5 to 6 m in the illite-smectite/kaolinite ratios which interval, which may reflect the short eccen is interpreted to be due to climatic fluctua tricity of 100.000 years. Variations are most tions. These have thus been obviously trig- 94 gered by shifts of the detrital composition Galerires roemeri is the "Opoka" facies of and not by changes in carbonate Ahlten, which overlies the Teutonia I sec bioproductivity (REHFELD et al., in press). tion (see above). There, probably in re A striking correspondence can be observed sponse to ecofacies factors, the Galerires between K/ Al maximum ratios and lineages developed an unmistakable ecoevent beds. If ecoevent beds should turn morphotype with features that significantly out to match climatic, Milankovitch-in differ from those of the marl-limestone duced variations, they would provide an facies of Misburg. The variability of the invaluable tool in tracing such cyclicities Misburg populations of the "vulgaris" Zone within sedimentary successions. is remarkable. Along with forms which re Cycle 8 contains only 3 marl beds and is semble G. sulca toradiarus, forms like G. distinctly thinner bedded than the subja globosus (sensu RoEMER non DEFRA.NCE) and cent cycles 2 to 7. It grades into the bed morphotypes with a conical corona (ERNST ded calcareous marl facies of superjacent 1975), co-exist. Thus, the terms G. vulgaris unit 2 (cycle 9), which is about 20 m thick Zone and G. roemeri Zone here may be and only faintly differentiated into marl equally unsuited to characterize this inter and limestone beds, though orbital forcing val. cannot be proved. Micrasrer (lsomicrasrer) stolleyi, the second Cycle 5 has been investigated by means of index echinoid, is an easily identified dis a "Croma-Meter" to determine the bright tinct form, which ranges from the stobaei/ ness in order to define the differences be basiplana to the minor/ polyplocum Zone tween calcareous and marly layers cor (Fig. 59). However, it is only at the base of rectly. Calibrated by geochemical carbon the vulgaris! basiplana Zone, that this in ate analyses (RFA), the carbonate content dex echinoid becomes more abundant. At of a layer can be easily determined by this least as a secondary index fossil, this method. The "Croma-Meter" has a bright echinoid turns out to be of value for intra ness index range between nearly 100 (pure European correlations, for example with white) to 0 (black). Within cycle 5 the in Spain. dex shows values in the marl layers which With respect to the ammonites, rare vary between 50 and 60, whereas the lime pachydiscid species (P. cf. haldemsis) may stone beds are characterized by signifi become important for the characterization cantly higher values, ranging up to 87 .It is of the " vulgaris" /srolleyi Zone (Fig. 64). The noteworthing that the brightness index and belemnitellids are in urgent need of restudy thus the carbonate content within the thick after CHRISTENSEN (1995) provided a quite middle bed increases towards the top. confusing revision of this group. Along with large forms, which may possibly be as Macrobiostratigraphy: Only few signed to Belemnirella woodi, small transi stratigraphic details will be given here, tional forms with large fissure angle appear treating only the highest parts (Upper in the higher portion of the zone, the lat Campanian "vulgaris" I stolleyi and minor! ter woud have been formerly assigned to polyplocum Zones) of the Teutonia I sec Belemnirella minor. tion. The base of the minor! polyplocum Zone The assignment of the "vulgaris"/stolleyi does not correspond to the distinct change Zone to the echinoids Galerires "vulgaris" in facies. It is drawn at the above-mentioned and Micrasrer (lsomicrasrer) stolleyi is event bed at the top of cycle 7 (bed K7 e; provisonal and urgently needs revision. Fig. 62), since a specimen of the This zone was termed the "vulgaris heteromorph ammonite Nosroceras Subzone" by KHOSROVSCHAHIAN ( 1972) and the (Bosrrych oceras) polyplocum has been in "obere vulgaris-Subzone" by ERNST (1975). ferred to come from this horizon (NIEBUHR Initially, ScHULZ et al. (1984) likewise used 1996a). Accurately horizoned specimens the term "vulgaris Zone" for this interval are first recorded somewhat higher in the in the standard section of Ui.gerdorf. Fol section in unit 9 (Fig. 62: beds d-j ), which lowing a revision of the genus Galerires, also yields abundant baculitid and Hu vulgaris scaphitid ammonites. Additional ammo Sc LZ ( 198 5) replaced the Zone by the Galerires roemeri Zone. In the opinion nites of this zone are ]elerzkyces of the authors, this revision is not justified. compressus, Hoploscaphires greenlandicus Type locality and stratum typicum of and Tra chyscaphires pulcherrim us (NIEBUHR 95 1995, 1996a). According to the former in type specimen), respectively, mostly small, dex ammonite, a compress us Zone has been slender forms appear with the internal coined in the scaphitid stratigraphy. The structures of B. minor (sensu German au first occurrence of the index species cor thors). re sponds to the unit 2 of the lower minor/ Echinoids are represented throughout by polyplocum Zone (NIEBUHr 1996a; see Fig. Micraster sp. of the main lineage and M. 64). Exi teloceras bipunctatum, indicator of (lsomicraster) stolleyi, which are missing the higher Didym oceras donezianum Zone in the "Opoka" facies of Ahlten. Galerites of Poland (BIASZKIEWICZ 1980) is absent in the "vulgaris " continues to be enriched in cer Teutonia I section since it characterizes the tain beds and no forms transitional to G. younger "Opoka" facies of Ahlten (NIEBUHR roemeri of the Ahlten "Opoka" facies oc 1995, 1996a; NIEBUHR et al. in press). cur. However, a first occurrence of The bostrychoceratids, so far collected, Cardiaster cordiformis announces the en have been assigned to the subspecies try of new echinoid assemblages in unit 2. Nos toceras (B.) polyplocumpol yplocum, N. (B. ) polyplocum unitubercula tum and N. References: BLASKIEWICZ ( 1980); (HRISTENSEN (B. ) polyplocum cf. secoense sensu (1995 ); ENGELHARDT (197 3 ); ERNST (197 5 ); BLASKIEWICZ (1980) and KOCHLER (in press). KHOSROVSCHAHIAN ( 1972); KOCHLER (in press); They are mostly preserved as fragments MILANKOVITCH ( 1941 ); MULLER & fABRICIUS and rarely yield more than one or two (1974); NIEBUHR & PROKOPH (in press); NIEBUHR whorls. ( 1995, 1996 ); NIEBUHR et al. (in press); RI:HFELD The belemnitellid fauna of this zone shows et al. (in press); ScHULZ (1985); ScHuLz et al. a significant turnover. Along with several (1984); ULBRICH (1974). large Belemnitella woodi or B. minor (sensu 97 2.13 Resse clay-pit (Figs. 65-72) Ammonites of biostratigraphic importance (by ]. Mutterlose) (Figs. 6 7-71) occur throughout the section. The concretions, in particular, yield rich Location and grid reference: TK 25, ammonite faunas which allow a detailed zo 3523 Garbsen, R: 3534900, H: 5816500. nation. The beds are dated as early Late The clay-pit is situated about 20 km north Hauterivian (upper part of the of Hannover directly west of the road from Aegocrioceras Beds and lower part of the Engelbostel to Resse (Fig. 2 ). This pit, which Simbirskites staffi ammonite Zone). has been operated since 1993, offers a good The lower part of the section (beds 94, 96, exposure of mid-Hauterivian claystones. 97, 98 and 100) is extremely rich in am monites. The genus Aegocri oceras is re Tectonic setting: The section is situated stricted to the lowermost part of the sec in the centre of a narrow E-W striking tion (beds 92-97) and has its last occur graben structure of about 1 5 km length and rence (LO) in the lower part of bed 97. 2 km width. The beds dip at 10° towards Aegocrioceras ra ricostatum (common in NW. bed 94) and Aegocrioceras spathi (common in bed 96) have been observed. The first Palaeogeography: Central pan of the NW Simbirskites were found in bed 96, German Basin about equidistant from the Simbirskites concinnus and Simbirskites Hildesheim Peninsula to the south and the decheni have been recorded from bed 98. Pompeckj Block to the north. The distances Bed 100 is characterized by the first occur towards each of the landmasses did not rence (FO) of Simbirskites staffi , the index exceed SO km. During the Hauterivian the species of the staffiZone. The heteromorph paleogeography was fa irly stable. A sea-way towards the Tethys via Poland (Carpathian Resse 0 sea-way) existed for most of the time, al 1: 0 . ... lowing floral and faunal exchanges. It is Cl) ii Cl) 1: 'Q. ::::I en only in latest Hauterivian time that the con ftl 1: '=,E..5! U) 0 - Cl) Ill 0 figuration changed considerably (compare N Lithology ::E m m o CaC03% 0 5 10 15 Frielingen, No. 14). 107 ------... Lithology and stratigraphy: 13 ... About • - m of clays and marly clays of early Late ., :.-:::-:::- ::: ------:::-t- Hauterivian age are exposed (Fig. 64). This 1: ., pit offers currently the only section of the • - Aegocrioceras/ ea - formerly well exposed ... :::-:::-:::-:::-:::- 10 Simbirskites "' =-===-- ======�--- junction beds in NW Germany. ·-... - - -- > �- -=&= - -= -= - : The lithology consists of dark to medium .Q - - -- =::=-=-=-=:- E grey claystones, the carbonate content is ... - Cl) generally low. CaCO, values vary between Cl) ==�======- 0.3% (sample 105/2 ) and 15.4% (sample - - -- - 102/1 ). In contrast to outcrops fartherwest, :I - �Q--=��--�------no sideritic nodules have been observed in ea - - -:-J!:-:::-: this section. Various horizons, however, - - - -- J: yield small calcareous nodules which com --=-=-=-=- 5 monly contain ammonites. The thickness -::::::::::::::::::::::::r- of these beds varies between 0.1 and 0.2 ... m, but they seem to be continuous. While Cl) ai coarser-grained clastics (silt) are generally a. Ul a. • absent in both the clays and the marls, ... - - - -- .. some of these horizons are characterized :::1 \) 0 -- - 100). ·;:: ------by a distinct silt content (bed Small \) ---- - 0 - pyritized burrows and pyrite nodules oc 1:11 ======.. ======"'{ = 1 cur throughout the sequence. Pale-dark -- - - - bedding rhythms (compare Frielingen, No. 14) are present, but less conspicuous than Fig. 65. Lithology and biostatigraphy of the Resse in other sections. section. 98 Haste 11 Haste IV Res se __ ...J r- c) ===== 25 6" 0: r- Lithology , m � i: !!! .. .. -----_ 20 � �.. 55 � 0: .Q ��-n r- ! 5� • Ill r- > s . .. A. J ------A.------...... �u • c. -=-=-= '15. -=�=�= �-15 1cs ��-t-1 m #::i�=t1 :::::::: - .. - - - 109 - ---5 �-+-T, 0 � ::12[ �33 Aegocrioceras ...... �� r- A spp. 10:: 3' Crioceratites hildestense r- c lQ·, ....=.. Stmbirskites ...... -.... =..::o spp Simbtrskites stalfi s5 - Fig. 66. Correlation of the Aegocriocers!Simbirskites junction beds of the Resse, Haste and Haste IV sec 11 tions (from MurrERLOSE & WrEDENROTH 1996). ammonite Criocera tites hildesiense has its the staffi Zone by the FO of S. staffi. The FO in bed 96 and occurs sporadically in Aegocrioceras Beds correspond to the the upper part of the section. Sim birskites (Speetoniceras) inversum Zone Apart from belemnites (Hibolithes in England. Since only a few specimens of jaculoides), bivalves (Nucula sp., Thracia the index species S. inversum have been phillipsii), gastropods (Turbo sp.) and crus observed in Germany, the traditional name taceans (Mecochirus ornata), remains of Aegocrioceras Beds is preferred over the fishes and marine saurischians have been inversum Zone. If the most recent proposal observed. The foraminifera are of low di (MurrERLOSE 1996) for defining the Lower/ versity and low abundance. Upper Hauterivan boundary by the LO of the nannofossil species Cruciellipsis Biostratigraphy: The ammonites from cuvillieri were be accepted, the base of the the Resse section supplied new important Upper Hauterivan would lie at the top of information about the faunal succession of the Aegocrioceras Beds. the Aegocrioceras /Simbirskites junction The old German zonation scheme, valid beds. In addition to the Resse section new until 1971, subdivided the interval under ammonite finds have been made recently discussion into a lower Aegocrioceras in the Haste sections, about 20 km west of capricorn u Zone and an upper Resse. Criocera tites hildesien se Zone (e.g. Traditionally, the lower Upper Hauterivian BARTENSTEIN & BETTENSTAEDT 196 2). The is subdivided into the Aegocrioceras Beds capricorn u Zone corresponds to the and the Sim birskites staffi Zone. The base Aegocrioceras Beds of the current scheme, of the Aegocrioceras Beds is defined by the the base of the hildesiense Zone was de FO of the genus Aegocrioceras, the base of fined by the FO of the heteromorph am- 99 ..-- / 2 \ �----�-.... 5 Fig. 6 7. Endemic ammonites from the Late Hauterivian Aegocrioceras Beds. 1. Aegocrioceras capricornu, Haste 2 section. 2. Aegocrioceras quadratum, Haste 2 section. 3. Aegocrioceras spa thi, Resse clay-pit, bed 94. 4. Aegocrioceras spathi, Resse clay-pit, bed 96. 5 . Aegocrioceras raricostatum, Haste 2 section. Specimens from the collection of K. WIEDENROTH. All figures are 1. x 100 \ \ ' \ \ \ 1 Fig. 68. Endemic heteromorph ammonites of the genus Aegocriocerasfrom the Late Hauterivian Aegocriocera.� Beds, demonstrating the great variation of coiling within the genus. 2 . Aegocrioceras ra ricostacum, Resse clay-pit. 1 . Aegocrioceras sp., Haste 2 section. Specimens from the collection of K. WIEDENROTH. Both figures are 0.5. X monite species C. hildesiense. The base of ammonite genera under discussion (Fig. 72; the C. hildesiense Zone and of the S. staffi MUTIERLOSE & WIEDENROTH 1995, 1996). Zone have approximately the same age. Both the Haste 4 section and the Resse sec There are, however, only few reliable data tion exhibit partially overlapping occur available from condensed sections along rences of Aegocrioceras, Criocera tites and the basin margin (Moorberg: BAHR 1964; Simbirskites. In Haste 4, Aegocrioceras spp. Speeton: RAwsoN 1971). and Crioceratites hildesiense eo-occur in The most recent finds from Resse and bed 42. Higher up in bed 44 these taxa eo Haste-both are expanded sections-now occur with S. (M. ) concinnus and S. (S. ) clearly demonstrate an overlap of the three decheni. It is noteworthy that S. (S. ) staffi 101 - ..... ·- -...c.· . -\; ·\ 3 4 Fig. 69. Ammonites of Boreal provenance from the Late Hauterivian Aegocrioceras Beds. 1. Simbirskites (Simbirskites J ex gr. decheni. Resse clay-pit. bed 98. 2. Simbirskites (Milanowskia) staffi, Haste 3 section. 3 . Simbirskites ( Milanowskia) concinnus, Resse clay-pit, bed 98. 4. Simbirskites ( Milanowskia) sp., Haste 3 section. Specimens from the collection of K. WIEDENROTH. All figures are x 1. has its FO even higher, in bed 48. Similar Three different possibilities for subdivid observations have been made for the Resse ing the Aegocriocerasl 5imbirskicesjunction section: Aegocrioceras spp. eo-occurs with beds result from these observations. The both C. hildesiense and 5. concinnus and base of the first 5imbirskices zone above 5. decheni in beds 96 and 97. The FO of 5. the Aegocrioceras Beds may be defined as scaffiis definitely younger, it has been first follows: observed in bed Fig. 71 gives a com LO of the genus Aegocrioceras. Following 100. • prehensive overview of the stratigraphic this definition, the Aegocrioceras Beds ranges of the sections and ammonites dis represent a full range zone, which yields cussed. in its upper part species of the genus 102 ,·, ! -�/ Fig. 70. Ammonites of Tethyan provenance from the Late Hauterivian Aegocrioceras Beds. 1. Criocera eites ex gr. duvali, Haste 3 section. 2. Spitidiscus rotula, Haste 2 section. 3,4. Spitidiscus rotula, Res se clay-pit, lateral and ventral view. Specimens from the collection of K. WIEDENROTH. All figures are 1. x Simbirskites (S. concinnus, S. decheni). concinnus-staffiZone. The interval under This proposal does not define the inter discussion is hatched in Fig. 72 (2nd pro val between the LO of Aegocrioceras and posal). the FO of S. staffi. In Fig. 72 (1st proposal) FO of Simbirskites staffi. This definition • this undefined interval is stippled. does not define the interval from the LO FO of the subgenera S. (Milanowskia) and of Aegocrioceras to the FO of S. staffi. In • S. (Simbirskites). In this case, the bound Fig. 72 this interval (3rd proposal ) is ary would be defined by the FOs of S. (M. ) hatched. concinnus and S. (S. ) decheni, somewhere below the FO of S. staffi. The problem with Migration of ammonites: The this suggestion lies in the absence of the En democeras/ Aegocrioceras junction beds index species S. staffi in the lowermost are characterized by an immigration of part of the eponymous zone. The addi Tethyan ammonites ( Criocera tites, tion of a new S. concinnus or S. decheni Olcostephanus, Spitidiscus) and Boreal gen Zone between the Aegocrioceras Beds and era (Simbirskites, Sp eetoniceras). This eo the S. staffi Zone does not make sense, occurrence of Tethyan and Boreal ammo since the intervalcovered by this zone is nite taxa within one bed has been demon extremely small. A possible solution might strated for the intervalC8A, C7H at Speeton be to rename the S. staffi Zone the S. by DoYLE (1989). This interval may repre- 103 � 3 . �ty: ....---t . .. . �.. �""" .. , . ... 4 Fig. 71. Ammonites from the Late Hauterivian Aegocrioceras Beds, Niedernwbhren section. 1. Aegocrioceras sp. 2. Aegocrioceras capricornu 3. Aegocrioceras capricornu 4. Aegocrioceras raricosca rum 5. Simbirskices (Milanowskia) scaffi. Specimens from the collection of K. WIEDENRonJ. All figures are 0. 75. x 104 Ammon1te Ammonite zones Old zonation New zonation ranges proposal proposal proposal STAGE NW Europe STAGE before after 1. 2 3. 1971 1971 NW Germany S. staffi S. staffi S. staffi Simbirskites (C.) discofalcatus Crioceratites Simbirskites hifdesrense staffi :;; Simbirskites (C.) gottschei D. � '/- 1 z D. z ::;) z .. Simbirskites (M.) staffi � I ;:� ;: D. �� D. c. .. AegoctiocetBs Simbirskites ::;) spp. a: � � '(;; a: Aegocrioceras AegocriocetBs Aegocrioceras Aegocnoceras Aegocnoceras w w ... I ... capncomu Beds Beds Beds ::;) EndemocetBs regalein�{',;�m ::;) -� � � Beds � � � - :z: :z: . � � � Endemoceras noricum "' . "("' � § � 0; Acsnthodiscus EndemocetBs ..I :;;it E. tBgale regale E. regale EndemocetBs smblygonium bivirgatus regale 0 E. ..I endemic taxa = telhyan taxa - boreal taxa 1nterval of taxa with m1xed -=--=-::� provenance 7 2. Proposals for the ammonite zonation of the early Late Hauterivian of Europe (from MurrERLOSE & Fig. NW WIEDENROTH 1996). sent a maximum flooding surface. The following species have been found in the Simbirskites 2, Boreal-Arctic species Haste Haste 4 and Resse sections: (Speetoniceras) inversum is common in the Aegocrioceras spathi, Aegocriocera s Aegocrioceras Beds of Speeton (RAwsoN bicarinatum, Aegocrioceras capricorn u, 1971; DoYLE 1989), in NW Germany it has Aegocrioceras compressum, Aegocrioceras been observed only in the lowermost quadra tum, Aegocrioceras raricostatum, Aegocrioceras Beds (KEMPER et al. 1987). S. Aegocrioceras semicinctum. Obviously this inversum is more common in the western endemic group underwent a rapid evolu part of the NW German Basin (Bentheim, tion in the Boreal Realm. Ammonite gen Teutoburger Wald, Niedernwohren), only era of a Tethyan or Boreal provenance are a few specimens have been recorded in the extremely rare in these beds. This pattern eastern part of the basin (Moorberg sec changes in the uppermost Aegocrioceras tion). This indicates an immigration of S. Beds: Criocera tites hildesiense and C. in versum from the NW via the Netherlands. duvali, two heteromorphs of Tethyan ori In NW Germany, the Aegocrioceras Beds are gin, are the first forms to immigrate. A dominated by the heteromorph slightly later immigration of Boreal Aegocrioceras, which is extremely abun Simbirskites is documented by the occur dant in this interval. The origin of this rence of S. concinnus and S. decheni. S. group, which is also common at Speeton is staffioccurs even later. According to RAwsoN still unclear (for discussion see RAwsoN & RILEY (1982) and RAwsoN (1994), the en 1975, 1995; lMMEL 1979; KEMPER et al. 1987). tire early Late Hauterivian is characterized Since Aegocrioceras is not known from the by a sea-level rise. Tethyan and Boreal ele Tethys, it is a genus endemic to the North ments eo-occur in this interval. Sea area. KEMPER & WIEDENROTH ( 1987) inter Thus, both the base and the top of the pret Aegocrioceras as a stenotherm cold wa Aegocrioceras Beds are characterized by a ter genus, RAwsoN (1995) derives this en eo-occurrence of Tethyan and Boreal am demic Boreal group from Tethyan monite faunas, reflecting two short-termed Criocera tites. Up to now only two specimens transgressive pulses. This would imply that of the Tethyan species Spitidiscus ro tula sea-level changes were the main factor con have been recorded from the Aegocrioceras trolling the biogeographic distribution pat Beds of Haste and Resse (MuTTERLOSE & tern of ammonites. WIEDENROTH 1996). Aegocrioceras is quite abundant both in the References: BAHR (1964); BARTENSTEIN & basin (Niedernwohren, Haste and Resse BETTENSTAEDT (1962); 00YLE (1989); IMMEL sections; MUTTERLOSE & WIEDENROTH 1996) and (1979); KEMPER & WIEDENROTH (1987); KEMPER in the basin margin (Moorberg section; et aL. ( 1987); MUTTERLOSE & WIEDENROTH ( 1995, KEMPER et al. 1987). The remaining fauna is 1996); MuTIERLOSE (1996); RAwsoN & RILEY extremely impoverished in the basin. Fol (1982); RAwsoN (197 1, 1975, 1994, 1995). lowing the revision of RAwsoN (1975) the 105 2. 14 Frielingen clay-pit (Figs. 73- beds between 12% (sample 119/1) and 53% 90) (sample 121/1 ) These pale-dark bedding . (by j. Mutterlose and A. Ruffell) rythms (P-D rhythms) are extremely well exposed in this pit and offer a good Location and grid reference: TK 25, possiblity of detailed studies. 3523 Garbsen, R: 3534900, H: 5816500. Small calcareous nodules, which rarely in The clay-pit is situated about 20 km north clude ammonites, are common throughout west of Hannover, directly east of the the sequence. The thickness of these lay BundesstraR.e B6 (Fig. 2). Between 1993 and ers varies between 0.1 to 0.2 m and they 1995 this pit expanded rapidly towards the appear to be continuous. Small pyritized west. burrows and pyrite nodules occur through out the section. Tectonic setting: The pit is located at Chondrites burrows occur at several levels the westernmost margin of a narrow E-W and are quite distinctive. Further ichnotaxa graben. This structure, which has a length observed include Planolites and of 15 km and a width of 2 km, runs paral Th alassinoides. lel to the southern flank of the Neustadt One horizon (bed No. 122) is rich in or salt dome. The beds dip at 15° towards ganic carbon and represents a forerunner WSW, the strike is 150°. of the Barremian Blatterton facies, depos- Palaeogeography: Frielingen lies in the Friellngen central part of the NW German Basin equi .. .. distant from the Hildesheim Peninsula to 1:0 0:: .!!! 0 TOC % the south and the Pompeckj Block to the Ill N north. Despite changing sea-levels, the 10 20 0.5 1,0 landmasses were never more than 50 km away. The palaeogeographic configuration during the Hauterivian was fairly stable. A sea-way towards the Tethys via Poland (Carpathian sea-way) existed for most of the time, allowing floral and fauna! ex changes. It is only in latest Hauterivian time (Simbirskites discofalca tus 0:: Zone) that the • palaeogeography changed. At this time, the Carpathian sea-way was closed and the NW > German Basin became the southernmost .. extension of the Boreal Arctic Sea with no .. " sea-way towards the south. However, .. slightly earlier in the Late Hauterivian Simbirskites discofalcatus Zone a transgres • 0 sion caused an influx of Tethyan derived nannofossils. This is supported by recent finds of Tethyan-derived bryozoa and Cl Ill foraminifera, which were observedin sam a. ples from the Frielingen pit (HEINRICH 1991; a. KLEIN & MUTIERLOSE in press). Lithology and stratigraphy: About 20 m of clays and marly clays of latest Hauterivian age (Simbirskites discofalcatus Zone) are exposed (Fig. 7 3 ). Dark to me dium grey claystones alternate with pale grey to whitish marls. CaC03 values in gen eral vary between 5% (sample 114/1) and 53% (sample 121/1). The dark beds show Fig. 7 3. Lithology and stratigraphy of the Frielingen a variation of CaC03 between 5% (sample section. The stippled intervals indicate the position 114/ 1) and 23% (sample 126/1), the pale of the detailed sections shown in Figs. 84, 85 and 88. 106 74. SEM photographs of foraminifera from the Late Hauterivian discofalca tus Zone, Frielingen clay-pit. Fig. 1. Meandrospira washicensis 200. 2. Meandrospira washicensis 182. 3. Hech cina anciqua 40. x x x 4. Globulina prisca, fistulas, 68. 5 . Linguloga velinella sigmoicosra, umbilical side, 59. x x 6. Lingulogavelinella sigmoicosca, spiral side, 58. 7.Pyr amidulina paucicosca 52. 8. Pyramidulina scepcrum x x 52. 9. Margin ulina pyra midalis 50. 10. Laevidenralina linearis x 23. 11. Episcomina caracolla, umbilical x x side, 3 7. 1 2. Ep iscomina caracolla, right coiled, 41. 1 3 . Ep iscomina caracolla, left coiled, 3 7. 1 4. Lenriculina x x x muensceri 31. 15. Leneiculina roemeri 30. 16. Leneiculina aff. pulchella 67. x x x 1 7. Lenciculina dunkeri 43. x 107 Fig. 7 5. SD-I photographs of foraminifera from the Late Hauterivian discofa/catus Zone, Frielingen clay-pit. 1 . Saracenaria pyra midaca x 93. 2. Astacolus aff. barrem ianus x 23. 3. Astaco/us bronni x 44. 4. Marginulinopsis gracilissima x 59. 5. Lenticulina eichenbergi x 27. 6. Marginulinopsis jonesi x 52. ? 8. Planularia tricarinella 42. 9. Psilocitharella strigilata bettenstaedti x 9. 1 0. Bullopara laevis on Citharina 7, x stria tu/a 11. Citharina acuminata x 29. 12. Citharina harp;� 40. 1 3. Citharina discors discors 15. x 8. x x 1 4. Frondicularia hastaca 26. 15. Frondicularia concinna 29. 16. Psilocitharella kochi prolaevis 12. x x x 1 7. Ps ilocitharella kochi kochi 22. 1 8. Ps ilocitharella trunca ta x xi S. 108 Fig. 76. SEM photographs of bryozoa (1-5) and foraminifera (6-14) from the Late Hauterivian discofalcacus Zone, Frielingen clay-pit. 1. Berenicea ten uis 14. 2. Berenicea tenuis 11. 3. Clinopora sp. x x 13. 4. Berenicea ten uis 26. 5. Berenicea tenuis small specimen 26. 6. Reophax scorpiurus 46. x x x x 7 . Proteonina ampullacea 122 . 8. Haplophragmoides cushmani 79. 9. Haplophragmoides concavus 70. 1 0. Haplophragmium aequalex 15. 11. Ammobaculites subcretaceusx 60. 12. Ramulina aptiensis x 35. x x x 1 3. Vern euilinoides neocomiensis 52. 14. Fa lsoga udryinella sp. 175. x x 109 �- : ' Fig. 77. SEI\1 photographs of calcareous nannoplankton from NW Germany. The bar in the lower right corner equals micron. 1. Vekshinella scradneri ssp., Late Hauterivian discofa/cacus Zone, Gott clay-pit, bed 57. I 2. Vekshinella sp., Late Hauterivian discofa/cacus Zone, Frielingen clay-pit, bed 117. 3. Vekshinella sp., Late Hauterivian discofa/catus Zone, Frielingen clay-pit, bed 117. 4. Biscucum conscans, Late Hauterivian discofalcacus Zone, Frielingen clay-pit, bed 117. 5. Biscutum conscans, Late Hauterivian discofalcatus Zone, Frielingen clay pit, bed 117. 6. Crucibiscutum salebrosum, Late Aptian nuclieldiensis Zone, Gott clay -pit Gott , bed 203. 7. /llicranrholiChus obtusus, Late Hauterivian discofalcatus Zone, Frielingen clay-pit, bed 117. 8. Micranrho/ichus obcusus, Late Hauterivian discofa/cacus Zone, Frielingen clay-pit. bed 117. 9. Manivirella pemmacoidea, Late Hauterivian discofalcatus Zone, Gott clay-pit, bed 57. 110 Fig. 7 8. SEM photographs of calcareous nannoplankton from NW Germany. The bar in the lower right corner equals 1 micron. 1 .Grancarhabdus meddii. Late Hauterivian discofalcarus Zone, Gott clay-pit, bed 57. 2 . Crecarhabdus anguscifora rus, Late Hauterivian discofalca cus Zone, Gott clay-pit, bed 57. 3. Microscaurus chiascius, Late Hauterivian discofalcarus Zone, Gott clay-pit, bed 57. 4. Rhagodiscus aspcr. Late Hauterivian discofalcarus Zone, Frielingen clay-pit, bed 117. 5 . Rhagodiscus asper, Late Aptian nucfieldiensis Zone, Gott clay-pit, bed 203. Heavily overgrown specimen. 6. Rhagodiscus asper, Late Aptian nuclieldiensis Zone, Gott clay-pit, bed 203. 7. Perissocycl us plechocrerus, Late Hauterivian discofalcarus Zone, Gott clay-pit, bed 57. 8. Perissocyclus plechocrerus, Late Hauterivian discofalca rus Zone, Frielingen clay-pit, bed 117. 9. Zeugrhabdorus sisyphus, Late Hauterivian discofalca rus Zone, Gott clay-pit, bed 57. 111 Fig. 79. SEI\1 photographs of calcareous nannoplankton from NW Germany. The bar in the lower right corner equals 1 micron. 1 . Wa tznaueria barnesae, Late Hauterivian discofalcatus Zone, Frielingen clay-pit, bed 117. 2. Nannoconus circularis, Late Hauterivian discofa/ca tus Zone, Frielingen clay-pit, bed 117. 3. Nannoconus circularis, Late Hauterivian discofalcatus Zone, Frielingen clay-pit, bed 117. 4. Na nnoconus minutus, Late Hauterivian discofa/catus Zone, Frielingen clay-pit, bed 117. 5. Nannoconus circularis, Late Hauterivian discofalcatus Zone, Gott clay-pit Gott, bed 58. 6. Na nnoconus circularis, Late Hauterivian discofalcatus Zone, Frielingen clay-pit, bed 117. 7. Nannoconus circularis, Late Hauterivian discofa/ca tus Zone, Gott clay-pit, bed 58. 8. Nannoconus circularis, Late Hauterivian discofalcatus Zone, Frielingen clay-pit, bed 117. 9. Nannoconus circularis, Late Hauterivian discofa/catus Zone, Frielingen clay-pit, bed 117. 112 Frielingen 0 Q) z :; Cl Q) 0 ea § mal 0 Ci5 N CO (.) I c: tl) ea � ·:; ·� � :i � 0 ea (.) I .!!! 'b Qi 0. 0. ::::> u:i Fig. 8 0. Occurrence of ostracods in the Frielingen section. The shaded interval indicates the position of the detailed section shown in Figs. 84, 85 (from MunERLOSE, Lurrow & GRENDA 1995 ). ited under anoxic conditions (MunERLOSE & KLEIN & MunERLOSE in press) and belemnites HARDING 1987a). (MunERLOSE, PINCKNEY & RAwsoN 1987) from this pit have been studied in detail. Flora and fauna: Various groups of fos LuTAT ( 1990, 1995) studied palynomorphs sils, including palynomorphs (LUTAT 1990, (spores, pollen and dinoflagellates) from 1995), calcispheres, calcareous the Frielingen section. Of the dinoflagellates nannofossils ( MUTIERLOSE 1991a; MUTIERLOSE the Spiniferites/ Achomosphaera group is et al. 1 994), foraminifera ( HEINRICH 1991; most common, as it ranges between 9% 113 Fig. 81. Ammonites from the Late Hauterivian discofalcatus Zone, Frielingen clay-pit. 1,2. Simbirskites (Simbirskites) toensbergensis, lateral and ventral view. 3,4. Simbirskites (Craspedodiscus) juddi, ventral and lateral view. Specimens from the collection of K. WJWENRonJ. All figures are x 0.5. 114 3 4 1 2 5 6 7 Fig. 82. Ammonites from the Late Hauterivian discofalcatus Zone. Frielingen clay-pit. 1,2. Simbirskites (Craspedodiscus) discofalcatus, ventral and lateral view. 3,4. Simbirskites (Craspedodiscus) phillipsi, ventral and lateral view. 5 . Simbirskites (Craspedodiscus) discofalcatus. 6, 7.Simbirskites (Simbirskites) toensbergensis, lateral and ventral view. Specimens from the collection of K. WJEOENHOTH. All figures are 0.6. x Fig. 83 (opposite page). Belemnites of Tethyan (Hibolites) and Boreal (Acroteuthis) provenance from the Late Hauterivian discofalcatus Zone. Each specimen is shown in ventral (left) and lateral view (right). 1,2. Hibolithes jaculoides. Gott clay-pit. 3 , 4. Acroteuthis (Boreioteuthis) rawsoni, Frielingen clay-pit. 5 , 6. Acroteuthis (Boreioteuthis) ra wsoni, Frielingen clay-pit. 7,8. Acroteuthis (Boreioteuthis) ra wsoni. Frielingen clay-pit. 9,1 0. Acroteuithis (Boreioteuthis) stol/eyi, Gott clay-pit. 11, 12. Acroteuthis (Boreioteuthis) stol/eyi, Gott clay-pit. All figures are 1. x 115 116 (sample 102/1) and 35% (sample 106/2) 0 Frielingen c of the total content. Less common is the • • .. -a "' c E Cribroperidiniuml Apteodinium/ • a • caco,•;. lii N Lith. m "' TOC % Trichodinium group (sample 12111: 2%, 10 20 30 40 0.2 0 4 0.6 0.8 sample 112/1: 15.5%), Circulodinium spp., Ba tioladinium spp., Sys tema tophora 153 complicata, Dingodinium cerviculum and 151 Tra beculodinium quinquetrum. The Chlamydophorella spp. group is quite com 147 mon, it varies between 5% (sample 12411) 145 and 33% (sample 11311 ). The latter group 143 shows two distinctive maxima: the first 141 ranges from bed 108 to bed 115, the sec c ond from bed 118 to bed 122. • Variations in the composition of > dinoflagellate assemblages can be used to reconstruct sea-level changes. These fluc • tuations are more obvious in sections of the basin margin (Gott, Moorberg), but are still present in basinal sections like Frielingen. .. Assemblages dominated by Nematospha eropsis scala, ( Tra beculodinium quinquetrum resp.), .. Dingodinium cerviculum and ... Chlamydophorella spp. characterize sea ... level highstands. High abundances of Sys tematophora complicata, Ba tioladinium - spp., the CribroperidiniumlApteodi niuml Tri ch odinium Circulodinium group and 1--- spp. are, on the other hand, typical of sea 1--- level lowstands. The abundances discussed previously indicate a sea-level high for most of the Frielingen section, interrupted by a 84. Detailed log of a single pale-dark rhythm slight regre ssion in beds 115-1 18. Fig. Palynomorphs of continental provenance (bed 111-113) from the Frielingen section, demon strating fluctuation in carbonate and total organic vary between 6.5% (sample 118/5) and carbon content. 50.9% (sample 1141 1 ). Calcareous nannofossils (Figs. 77-79) are rich and diverse throughout the section species (30 agglutinated species, 91 calcar (MUTIERLOSE 1991a; MUTIERLOSE et al. 1994), eous species). The fauna is dominated by with both being highest in the pale beds. eight species (Ammobaculites subcretaceus, The most common species include Discorbis dreheri, Epistomina Wa tznaueria barnesae, Rhagodiscus asper, (Hoeglundina) caracolla, Falsoga udryinella Vekshinella spp., Corollithion spp., sp., Lenticulina (Lenticulina) muensteri, Biscutum constans, Crucibiscutum Lenticulina (Margin ulina) robusta, salebrosum and Sollasites horticus. Tethyan Pro teonina ampullacea, Vern euilinoides warm-water floras consisting of neocomiensis). Detailed studies were com nannoconids (N. kamptneri, N. circularis, pleted by HEINRICH ( 1990, 1991) and KLEIN & N. globulus, N. minutus, Nannoconus spp.) MUTIERLOSE (in press). are restricted to the pale beds and they are 29 taxa of ostracods were described from rare or absent in the dark beds. The rela the Frielingen section (MuTTERLOSE et al. tive abundance of Nannoconus varies be 1994), with the highest abundances in beds tween 0.3% to near 10% in the pale beds 96-100 and beds 107-113. (with a maximumabundance of 9.9% in bed The macrofauna includes species of the Simbirskites 117). Boreal ammonite genus (S. (Craspedodiscus) discofalca tus, Benthic foraminifera (Figs. 7 4-76) are gen S. erally rich and diverse. They consist of 121 (Simbirskites) picteti, S. (Simbirskites) 117 r F ielingen ci z ci "' D•versny ",o Zeugrhabdotus• spp "' "' 5 z c. CaC03 °/o B. constans 8 constans 010 C. salebrosum �o 5. hOt11CUS '}o g' c: lilh. 0 "0 E re 0 cm "' c?jo 4 4 u; u m 20 40 24 26 32 36 0 2 6 0 2 6 0 2 4 6 0 10 20 150 145 140 135 130 125 120 115 111 20 110 10 105 Fig. 8 5. Detailed log (bed 11-1 13) from the Frielingen section, demonstrating diversity and relative abun dance of calcareous nannofossils and carbonate content within a single pale-dark rhythm (from MurrERLOSE, LliPPOLD & GRENDA 1995 ). toensbergensis, S. (Craspedodiscus) juddii; of pale and dark colours in the field is Figs. 81, 82) and the Tethyan ammonite highly subjective, being dependent on the Criocera tites strombecki. The Tethyan water saturation of the rocks and on the belemnite Hibolithes jaculoides is quite intensity of the sunlight (amongst other fac common, it eo-occurs with the Boreal tors). belemnite Acroteuthis (A. (Boreioteuthis) Carbonate values vary between 12% (sam stolleyi, A. (Boreioteuthis) ra wsoni; Fig. 83 ). ple 119/1) and 53% (sample 12111) in the The brachiopods, which include pale layers, and between 5% (sample 114/ Terebra tulina martiniana, Rugitela rugosa, 1) and 23% (sample 126/1) in the dark lay Rugitela roemeri, Cyrtothyris sp. and ers. The average values are higher in the Lamellaerhyn chia rostriform is are of Boreal pale beds than in the dark ones. Organic affinities, typical of the North-Sea -north carbon varies from 0.3 to 1.7% most corg' German clay facies. In addition, crustaceans samples range from 0.5 to 0.9% The Corg· ( Callianassa uncifera), solitary corals, pale bed 121 shows the lowest cor value g serpulids and shark teeth have been ob (0.34%), the dark bed 124 the highest value served. Recently bryozoans (Berenicea) ( 1.7%). The Cor values for the dark beds were found in the pale beds 122, 124 and are in general sfightly higher (0.2 to 0.3%) 126. than those of the directly under- and over lying pale beds. Pale-dark bedding rhythms: The lithic A high resolution study (Fig. 84) clearly log, which is about 20 m thick, is charac shows that both carbonate and cor fluctua terized by typical bedding rhythms. These tions are gradual and can be lin�ed to li consist of 22 clay-marl rhythms, each of thology. these rhythms having an average thickness In the eastern part of the NW German Ba of about 0. 9 m. The visual differentiation sin clay-marl bedding rhythms have al- 118 c. c. c. cg. g. � g. 0 � � "' � c� � � �"" 0 �.c E � c <>.. g. !5c E .. � �0 c � ;:: a: � ll � < c A f•:•:•j marl - m Lithology � ----� clay Colour : D pale mediUm - dark Fig. 86. Detailed log (bed 111-113) from the Frielingen section, showing the ranges of calcareous nannofossils within a single pale-dark rhythm (from MUTIERLOSE, LUPPOLD & GRENDA 1995 ). ready been observed in the Early Rhagodiscus asper, Cretarhabdus spp.) are Hauterivian (Endemoceras amblygonium more common in the pale layers (Figs. 85- ammonite Zone). These bedding rhythms 87). These taxa indicate warm surface wa become most conspicuous in the ters, impoverished in nutrients. Dark lay Hauterivian/Barremian boundary interval. ers, on the other hand, impoverished in They are, however, absent in exposures CaC03 and enriched in show a relatively Corg' situated in the centre of the basin. Sections high percentage of Wa tznaueria barnesae, in the western part of the basin show dis Sollasites horticus, Corollithion spp. and tinctive Chondrites layers, which are ab Biscutum constans. The latter species is sent further west. common in cooler nutrient rich surface The distribution pattern of calcareous water and is taken as a proxy for a slightly nannofossils clearly shows two different higher productivity. The variation of cal sedimentary cycles superimposed on one careous nannofloras within each clay-marl another. These are recognizable both along rhythm may be best explained by climatic the basin margin (Gott section) and the variation on the scale of Milankovitch cy basin centre (Frielingen section). cles (precession and obliquity). These short Each one of the horizons within a single term variations reflect changes of surface pale-dark bedding rhythm shows a cyclic water temperature and fertility. variation of all parameters studied (CaC03, The foraminiferal diversity is generally cor ' distribution of calcareous higher in the pale beds than in the dark g nannofossils). Pale, marly layers are char ones. Meandrospira washitensis, a species acterized by a relatively high CaC03 and a of presumed Tethyan warm water affini low Cor content, respectively. Tethyan and ties, is common only in the pale layers g cosmopolitan floras (Nannoconus spp., (HEINRICH 1990, 1991; KLEIN & MurrERLOSE in Con usphaera, Micrantholithus spp., press). It is associated with the bryozoan 119 I 14 r------, I 12 �, o , = J., I I .t. aark. I o 'I pale e . I 0.25 i I � !I I ------I o�· 20 30 � I 10 40 so 10 20 30 40 so CaC01 % .. N(d�15 . C.CO,% N(p)� . N(d)Z1!i -�P)-40 20 �==�======� 2 0 ,------:------, c c )! 1.5 c 0 ·� � � tO . •dark : 6 •a: t"' ... cc. 0 cpale ti 0.5 ; ti 0.5 .t.OO C I I c 0 I 0,0 0.0 0�---___..J 10 40 -50 · ...� 20 .30. 0 2 4 6 8 10 12 1-4 R.- % Fig. 8 7. Relations between total organic carbon, carbonate content and nannofossil abundance within pale and dark beds of the Frielingen section. Berenicea, hitherto known only from the Frlellngen g Early Hauterivian reef facies further north g t east (Fig. 88). These observations support 'i � Lithology Ill Ill the inference that the pale beds were de 10 20 300 posited under warm surface water condi tions. Ostracod diversity is considerably higher in the pale layers compared to that in the dark layers (Fig. 80). Species with eye tu bercles and the thermophile genus Cy therelloidea are recorded among the ostracods within the pale layers. These oc 0:: currences suggest sedimentation in warm • water within the photic zone. > Superimposed on these small-scale rhythms are lower order cycles caused by longer sea B L=-�- I-- " II. B level fluctuations. A sea-level highstand in -_ -_- 1,5 ==�== 125 the middle part of the Simbirskites 11.B - 100 - discofalca tus ammonite Zone allowed an - }!;, I-- • - ...- - -- - influx of Tethyan genera and species. The � - �=-�- =� 1 24 3,6 regression in the late discofalcatus Zone - --'i" - -:i:==�--- = caused a dominance of the nannofossil spe "'i" x cies Biscutum constans. .. 1-- 0. Clay mineralogy: The results of a semi I-- quantitative analysis of the clay mineral ogy of the pale-dark rhythms shows that 3,2 pale (calcareous) beds contain abundant mixed-layer illite-smectites and always 122 some chlorite (RuFFELL in prep.). The pale beds contain crystalline smectite, illite and - · - -- - kaolinite in lesser amounts than the dark - --.. beds. By contrast, the dark beds contain illite and kaolinite in abundance with lesser Fig. 8 8. Detailed section (beds 122-12 8) from the Frielingen section, demonstrating the exclusive occur amounts of smectite and mixed-layer min rence of Tethyan derived foraminifera (M=M. erals. The variation in clay mineral abun- washitensis) and bryozoa (B) in pale beds. 120 dances between dark and pale beds is rarely Factor Factor Factor 1 2 3 more than 5% in any one mineral species, E. caracolla 0.930 -0.102 -0.035 and is significantly lower than the changes CaC03 0.787 0.072 -0.019 in the abundance of different clays f. calacareous 0.705 0.337 -0.538 throughout the Upper Hauterivian. agglutinated f. -0.705 -0.337 0.539 TOC It is important to place bed-by-bed changes -0.560 -0.444 0.138 in clay mineralogy in a regional context, in 0.168 0.820 0.113 M. washitensis order to understand the likely mechanisms F. tealbiensis 0.194 0.806 0.013 diversity -0.145 0.790 -0.162 controlling their abundance. The error margins involved in semi-quan P. ampulacea -0.448 -0.581 0.368 titative analysis of clay mineral populations D. dreheri 0.037 -0.150 -0.845 T. agglutinans -0.156 0.018 0.772 are potentially very high. In reconnaissance spp. Reophax -0.084 -0.268 0.732 studies of the clays of the Lower Cretaceous, it was found that different methods of cal culating mineral abundances could lead to a 5 to 10% variation in results. As bed-by bed variations rarely exceed this figure, overall trends in the clay mineral popula Factor 1 Factor 2 Factor 3 tion are taken as being more reliable than S. horticus -0.840 -0.136 -0.218 absolute values. In addition, due to the dif spp. Nannoconus 0.838 -0.152 0.037 ferent origin of clay mineral species, rela spp. Cretarhabdus 0.824 0.077 0.102 tive proportions are also thought to reflect CaC03 0.763 -0.451 0.260 more accurately the changes in the amount TOC -0.640 0.262 -0.541 of detrital clay minerals. C. margerelii 0.553 -0.466 -0.061 spp. Although the margins of error are high in Corollithion -0.528 0.476 0.397 B. constans 0.021 0.884 0.063 estimating absolute quantities of different R. asper 0.291 -0.806 0.195 clay mineral species in any given sample, spp. Vekshinella 0.168 0.710 0.498 the variations between pale and dark lay W. barnesae 0.045 -0.160 -0.929 ers observed here are consistent through 0. /ehmanii 0.370 -0.057 0.794 out the Hauterivian sections studied. The majority of pale layers contain abundant Fig. 89. Factor analysis of a Frielingen data-set con- taining foraminifera-, nannofossil-, carbonate-, and mixed-layer illite-smectites, pure smectite total organic carbon data. in some samples, and lesser amounts of kaolinite and chlorite than in the dark lay ers. This may indicate more "off-shore" conditions, when sea-levels were high, tec tonic uplands were low in relief and when the diagenetic alteration of illites and , , • cacoo· · a . 4 loC�F.�: � ----!. �-2 0.0 � �-6 .8 Factor2 ° 2 _4 � · 0 . �-2 -4 .Fad0r1c. 0.0 0.6 • · 0.2 Fader 2 0 o.e o.s ·4 Factor 1 Facia 3 1.0 1.0 °·8 N=34 Fig. 90. Factor analysis of a Frielingen data-set containing foraminifera-, nannofossil-, carbonate- and total organic carbon data. 121 smectites could occur, i.e. in a seasonally humid weathering regime, with hinterland arid climate. Dark layers generally show areas being actively eroded. high quantities of kaolinite, smectite, with a few samples containing mixed-layer min References: HEINRICH (1990, 1991 ); KLEIN erals and chlorite. This assemblage might & MUTIERLOSE (in press); LUTAT ( 1990, 1995); indicate more "near-shore" conditions, al MUTIERLOSE & HARDING ( 1987a); MUTTERLOSE ( 1991 ); MuTIERLOSE 1994 ); MurrERLOSE, though the presence of both smectite and et al. ( kaolinite might be better explained by a PINCKNEY & RAwSON (1987); RUFFELL (in prep.). 123 2. 1 5 M unchehagen quarry (Figs. 91- pression. The best overviewcan be obtained 96) from a viewpoint near the windmill of (by ]. Mutterlose) Bergkirchen, about 3 km east of the park. The beds within the quarry dip at 1 oo to Location and grid reference: TK 25, wards WSW. 3521 Bad Rehburg, R: 351370, H: 581210. The disused quarry is now the central part Palaeogeography: During the Berriasian of the "Dinosaurier-Freilichtmuseum the area now forming NW Germany con Munchehagen". It is situated about 20 km sisted of an elongate basin extending about northwest of Hannover, northeast of the 280 km in west-east direction and about village of Munchehagen (Fig. 2). 80 km from north to south (Fig. 91). To the south the basin was bordered by the Tectonic setting: Southwestern shoulder Rhenish Massif, where Carboniferous of the NW-SE Rehburg Anticline. The cen sandstones were exposed (BALDSCHUHN & tral part of this salt-induced structure is KocKEL 1994 ). Triassic sandstones and formed by evaporites of latest jurassic age mudstones were exposed to the east on the (Munder Formation, Tithonian), the south Netherlands High and, to the north and western and northeastern shoulders by northeast, the area was bounded by the Berriasian sand- and siltstones (German Pompeckj Block. Throughout most of the Wealden). Due to the massive sandstones, Berriasian the NW German Basin was sepa Berriasian strata are resistant to weather rated from the open ocean and brackish ing and thus form narrow elongated ridges and freshwater conditions prevailed. Sev (Rehburger Berge). Beds of Tithonian age, eral short-lived periods of marine flooding which form the central part of the anticline, are documented: in particular for the crop out around the village of Buckeberg Formation or upper Wealden 2/ Wiedenbrugge, forming a topographic de- lower Wealden 3 to upper Wealden 3/lower Localities: area of non-deposition/ e 15 Miinchehagen predominantly sandstones r·,_-:11 erosion clayey sediments clayey sedlments with I I (less than 400m thick) Intercalated sandatones clayey scdlments calcareous sedlments I I (more than 400m thick) Fig. 91. Palaeogeography of the NW-German Basin in Berriasian times (from ELSTNER & MUITERLOSE 1995). Compare also Fig. 6. 124 Wealden 4/lower Wealden 5 of the stand margin (in the area west of the River Ems) ard German lithostratigraphy (STRAuss et al. are characterized by Neomiodon limestones 1993). and mudstones that also extend furthereast These marine flooding phases are marked into the basin. This mudstone facies may by the presence of marine palynomorphs exceed 400 m in thickness in the eastern and fo raminifera ( STRAuss et al.199 3). The most part. marine incursions are presumed to have The central part of the basin is dominated come from the west via the East Nether by up to 700 m of mudstones. Sandstones lands High since marine influences become and Neomiodon limestones occur only less distinct towards the middle and east along the northern and southern rims, ern part of the basin. Similarly, both the where coarse-grained clastics were shed abundance and diversity of marine from the northern Pompeckj Block and microfaunas in these intervals diminishes southern Rhenish Massif. Local areas of towards the east. sediment accumulation were controlled by Facies distributions and different sediment narrow E-W basins, created by accumulation rates allow the NW German synsedimentary salt diapirism. There is a Basin to be subdivided into a western,cen general trend towards coarser clastic ma tral and eastern part (ScHorr et al. 1967, terial towards the east (marked in the east 1969). The sediments of the western basin by the present-day River Weser), where the 50 m 0 � ' ...... __ \ ·...: ., • " :. " ... ' } . ( / / I I " "" ...... I I I I I I I I ',� Fig. 92. Sketch map of the abandoned Miinchehagen quarry, today forming part of the "Dinosaurier Freilichtmuseum Miinchehagen" (modified after F1scHER & THIES 1993 ). 125 dominant fluvio-deltaic sands interdigitate most recent zonation scheme they can be with a variety of lithologies. This eastern assigned to the Cypridea alta fo rm osa area is dominated by sandstones, siltstones ostracod Subzone (ELsTNER & MuTTERLOSE and silty claystones. Neomiodon limestones 1996). Several massive sandstone horizons occur and coal seams are common. Two varying in thickness between 0.5 and 1 m different sandstone fans, both shed from are separated by thin clay layers with a the south, can be differentiated. The thickness of a few millimetres. The sand smaller, western fan is present in the stone itself is a hard, medium brown, fine Osnabruck area, the eastern one is devel grained quartz sandstone. The quartz oped in the Buckeberg-Hannover area. grains are embedded in a fine-grained ma The sandstones exposed in the trix. CHITSAZIAN ( 1985) studied the sandstone Munchehagen quarry are part of the east with respect to its petrography. Qu artz ern fan. The hinterland, situated about 40 makes up to 93 % (vol.), while rock frag km to the southeast in the Hils area, was ments ( quarzite, lydite, rare pebbles of ig characterized by the sedimentation of silty neous rock) make up about 2%(v ol.). Mus clays, siltstones and coal seams. These beds covite is not common and heavy minerals were deposited in a braided river system (tourmaline, rutile, zircon) are rare. They under a humid climate. North and west of make up about 0.3 % (vol.). About 5%(vol .) the Hils area these fluvial deposits are re are formed by the matrix. placed by thick, massive, non-marine The Rehburg Sandstone is a silty, fine sandstones with some coal seams. This so grained sandstone, having a maximum called "Wealden Hauptsandstein" forms a grain size of 50 to 60% between 112 and large fan covering the Buckeberge-Harrl 200 1..1m. Medium-grained components Deister-Rehburger Berge area. Sandstones make up 25 to 30%. According to these of this age have been observed as far east data, the Rehburg Sandstone can be classi as Sehnde, about 20 km east of Hannover. fied as a well-sorted sandstone with me Traditionally, this sandstone fan has been dium rounding. interpreted as originating from a delta Ripple marks, both oscillatory wave ripples shedding material from the south into the and current ripples, are common, the di basin (KAUENHOVEN 1927 ) . Recently, the rection of the crests varies within one bed. Wealden Hauptsandstein has been reinter Small-scale cross bedding can be observed. preted as a transgressive barrier sand de The basal bedding plane ("Sohlflache"), posited parallel to the coast-line (PELZER which is exposed all over the quarry, has a 1988). thickness of 0.1-0.2 m and forms the lowermost sandstone bed of the Wealden Lithology and stratigraphy: About 8 Hauptsandstein. About 1 m of shale and a m of grey to brown, fine-grained, thin- to coal seam 0.2 m thick underlie the basal medium-bedded sandstones are exposed. bedding plane (WILDE et al. 1995). The sandstones represent the lowermost part of the Wealden Hauptsandstein, and Macrofossils: Apart from ichnofossils, are part of the Wealden 3. According to the which are very common, particularlyon the ... z 13 15 9 17 5 Left 5 7 3 r:f";\ 0 �O(J}©) CGi� 21 0 e 0:> G 1 c� Cl:> 12 16�7:: ; �0 10 18 ..• Q � 8 \ Front Feet G> ()) � ��� 20 0 6 Right Back Feet 2 4 22 m �m�=c��=F�����=10����=F����=T2�0������:c:c� Fig. 9 3. Detail of a sauropod track (Track 5) from the Mi.inchehagenquar ry (modified after LooK et al. 1988). 126 observed in the former quarry. All foot 10 m prints are preserved as imprints on the 1 9 20 surface of the basal bedding plane and are •c 11 moving direction partly covered with sediment. On the basis 18 • 0 of shape and size, two main types are dis 15 • cernible: sauropod and three-toed imprints. 16 & (J 13 The following data is taken from FISCHER 14 • Right THIES (1993 ). Left Seven tracks (Figs. 92, 93) in the western O 12 part of the quarry show round to suboval or triangular imprints. About 256 of these imprints have been mapped. Track 5 is the .11 best preserved one, showing 22 footprints over a length of 80 m. The track consists of 100 two parallel rows of imprints, 13 of which . 9 10 show the imprints of both front and hind legs. The imprints of the front legs are a . - surface of the basal bedding plane, body . . fo ssils are very rare. Internal moulds of the bivalve Neomiodon ( = Cyren a) have been • observed,indicating fresh water conditions. Plant debris also occurs...... 10cm Ichnofossils: The basal bedding plane is characterized by ichnofossils of high abun dance and low diversity. Apart from the most spectacular dinosaur tracks, Th alassinoides, Muensteria, Planolites, Pelecypodichnus, Cubichnia and other taxa have been described by WILDE et al. (1995). These ichnofossil associations indicate a well-oxygenated environment with low sedimentation rates. The ripple marks must have formed under shallow-water condi tions. Dinosaur footprints: The most spectacu lar fossils are several tracks of dinosaur Fig. 95. Tridactyl footprints of bipedal dinosaurs (possibly Ig uanodon or Megalosaurus) from the footprints, indicating a non-marine envi "Wealden Hauptsandstein" (modified after HAUBOLD ronment. A total of 275 footprints has been 1984). 127 Lithostratigraphy Biozones and � NW Germany Lithology Subzones Age et: m Platylenticeras Beds W6 PI. robustum P. trapez.P. rotundata �w�=��l--c� _._pra�-a-"e=-'a_11/ (/) :::l W3 SO m P. t 0 compacta Q) 0 t ltl C. rectidorsataC. alta � fo�osa (.) c: W2 ---- "- 1------1 ltl -=-·==-·=·=- E.� C. bispinosa "iii -�Qj W1 C. altissima ID -s-.. � OM 6 c: � ��;;t=�faC�sciculatayp�n�de�a� j 1-'cn"--i---.. �E .o ::------:::: �C. posticalis ., u..0 ::2 !?' � �C.� binodosa OM 5 ----F� :- : : : : : g � ------Qj � - - - _ _-: 5. .!:; F. -t (j (j -g':::l ::.:: !.iJ -� � M. dictyota ...... ,... ::E ----- ansata -, OM 4 � M. macula/a claystone limestone coal seam � � rich shale sandstone unconformity C0,9 [3 Ti. Tithonian shelly limestone marl c=J J. Jurassic Fig. 96. Litho- and biostratigraphy of the non-marine Berriasian and basal Valanginian of NW Germany (from ELSTNER & MurrERLOSE 1996). lated, resulting in a body length of at least side of the leg. From this interpretation, we 5 m. As is indicated by the size of the im may then reconstructthe direction in which prints and the stride, track 5 was caused the animal moved: in the present case, these by the largest animal in comparison to the quadripedal animals all travelled from west animals that made the other tracks. All to east. these imprints were made by quadripedal, A second type of footprint (Figs. 94, 95) is "elephant-footed" sauropods. Movement of exposed over a length of 28 m in the south the animals from west to east is indicated eastern part of the quarry. 19 imprints, for all the tracks. In vertical cross-section made by a bipedal three-toed dinosaur the large footprints of the hind legs show a (possibly Ig uanodon or Megalosaurus), regular asymmetry, characterized by one form a track. The size of these imprints steep and one shallow side. The steeper varies between 0.44 and 0.56 m (length) crest is interpreted as reflecting the inner and 0.43 and 0.52 m (width). The average 128 stride is 2.51 m, the width is 1.22 m. Left It is less applicable in the sandy facies. and right-handed imprints can be distin guished by the orientation of the third toe. Palaeoecology: Sedimentologic features An overall body length of 7 to 8 m has been (cross bedding, ripple marks) and calculated, the animal's hip was about 2 m ichnofossil data clearly suggest deposition above the ground. of the basal bed in a shallow aquatic re gime. From the palaeontologic data a Biostratigraphy: The biostratigraphy of swampy fresh-water setting is most prob the non-marine Berriasian in NW Germany able. The bivalves observed (Neomiodon, is based on ostracods. A recent review of Unio) are clearly fresh-water taxa, and the the ostracod zonation has been given by dinosaur imprints indicate a shallow water ELSTNER & MurrERLOSE (1996). According to depth of up to 1 or 2 m. this most recent zonation scheme, the Wealden Hauptsandstein can be assigned References: BALDSCHUHN & KocKEL (1994); to the Cypridea alta formosa ostracod (HITSAZIAN ( 1 9 8 5); ElSTNER & M UTTERLOSE Subzone. It should be noted, however, that (1996); fiSCHER & THIES (199 3); KAUENHOVEN the ostracod zonation can be applied only (1927); PELZER (1988); SCHOTT et al. (1967, 1969); RAuss (1993); WILDE to the basin facies further tothe northwest. Sr et al. et al. (1995). 129 Acknowledgements: G. Ernst, ]. Mutterlose and K.-A. Trbger acknowledge financial support by the Deutsche Forschungsgemeinschaft (Er 29/20, Er 29/2 1, Mu 66 7/8, Tr 309/2-4), which allowed them to carry out most recent research in the Cretaceous. G. Ernst, B. Niebuhr, U. Rehfeld (Berlin) and C. ]. Wood (Croydon), are indebted to students of the working-group "Upper Cretaceous" (Berlin), who provided essential data of their Diploma theses. F. Horna would like to express gratitude to K.-A. Trbger (Freiberg), G. Ernst (Berlin) and T. Voigt (Jena) for many discussions and is really indebted to C. ]. Wood (Croydon) for improvements of the English. His studies were supported by a PhD stipend of the Studienstiftung des Deutschen Volkes. ]. Mutterlose thanks C. Klein, D. Nebe and M. Schaaf (all Bochum), who supplied impor tant informations from their Diploma- or PhD theses. K. Wiedenroth (Hannover) made biostratigraphic data available and provided specimens from his collection. P. Schulz (Berlin) and M. Ress (Bochum) took the photos. A. Bornemann and B. Niermeyer drew most of the figures, S. Rauer carefully formatted the references (all Bochum). The edi tors thank H. Friedrich (Bochum) for technical assistance in digital publishing. References: von Baddeckenstedt und Floteberg (Nieder ABtJ-MAARUF,M. 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