Тне Campanian-Maastrichtian Boundary in Тне Chalky Facies Close То Тне Тype-Maastrichtian Area

ТНЕ CAMPANIAN-MAASTRICHTIAN BOUNDARY IN ТНЕ CHALKY FACIES CLOSE ТО ТНЕ ТYPE-MAASTRICHTIAN AREA

Francis ROBASZYNSKI, Martin J.M. BLESS, P.J.(Sjeuf) FELDER, Jean-Claude FOUCHER, Odile LEGOUX, Helene MANIVIT, Jan P.M.Th. MEESSEN and Luit А. VAN DER TUUK

AOBASZYNSKI, F., BLESS. M.J.M.. FELDER. P.J.. FOUCHER. J.-CI .. LEGOUX. О .. MANIVIT. Н .. MEESSEN. J.P.M.Th. & VAN DER TUUK. L.A. (1985). - The Campanian-Maastrichtian boundary in the chalky facies close to the type-Maas trichtian агеа. - Ви/1. Centres Rech. Explor.-Prod. Elf-Aquitaine, 9, 1. 1-113, 35 fig .. 22 pl., Pau, June 28. 1985. - ISSN 0396-2687 CODEN BCREDP The рарег develops results related to the macro- and micropalaeontological content of the chalks known оп either sides of the Campanian-Maastrichti;эn boundary in the type-Maastrichtian агеа. This boundary is studied in the Halembaye quarry (NE of the Belgian Limburg) and in the агеа around Beutenaken (SE of the Netherlands Limburg). Analytical results аге presented for both Ьiostratigraphical and palaeoecolo gical aspects. Biostratigraphical evidence is given with the distribution of macrofossils. especially Belemnites and other Cephalopods. and of microfossils such as benthic and planktonic Foraminifera. Nannoplankton and Dinoflagellates. Palaeoenvironmental characteristics are suggested after quantitative study оп fossil groups giving good palaeoecological information such as mesofossils. Ostracods. Spores and pollen grains. Thus, from one of another fossil group. Ьiostratigraphical zones and ecozones are defined. The proposal Ьу the lnternational Subcommission оп Cretaceous Stratigraphy for beginning an extended Maastrichtian stage with the appearance of Belemnella lanceolata is followed up here. With this concept. the Zeven Wegen Member containing Belemnitella mucronata and Belemnitella mucronata "тinor" is considered as Upper Campanian. the Beutenaken Member with Ве/етпе//а /anceolata inflata and Ве/етпе//а "occidentalis" is lower Lower Maastrichtian, the Vijlen Member with Belemnitella junior is Upper Maastrichtian (lower part). Long absences of sedimentation separate the three members and are marked Ьу hardgrounds. but reworked material is present only at the very base of each member. The vertical distributions of macrofossils. Foraminifera. Nannoplankton. Dinoflagel lates. Spores and pollen grains. mesofossils and Ostracods are presented оп several charts and their stratigraphical and ecological value are commented оп. F Robaszynski. Faculte Po/ytechnique. lnstitut de Geologie. rue de Houdain 9, 7000 Mons (Belgium). - М.J.М. 8/ess and P.J. Felder, Natuurhistorisch Museum Maastricht, Bosquet-plein 7, 6211 KJ Maastricht (The Netherlands). - J.-C. Fou cher, Facu/te des Sciences de /'Universite. Laboratoire des Sciences de /а Terre, В.Р 347, 51062 Reims CEDEX (France). - О. Legoux, SNEA(P), Laboratoire de Geologie, Departement Biostratigraphie. Boussens, 31360 Saint-Martory (France). - Н. Manivit, BRGM and LA 319 Paris VI, В.Р 6009, 45060 Orleans CEDEX (France). - J. Р.М. Th. Meessen, Geologica/ Survey of the Netherlands, Geologisch Bureau,

РЬ. 126, 6400 АС Heerlen (The Netherlands}. - LA. Van der Tuuk, Flamingostraat 20. 3582 SX Utrecht (fhe Netherlands). Кеу words : Boundary. Campanian. Maastrichtian. Biostratigraphy. Belemnites. Stra totype. Netherlands (Beutenaken). Belgium (Halembaye quarry). Limburg.

RESUME CONTENTS

La limite Campanien-Maastrichtien est etudiee dans 1. INTRODUCTION ...... 3 le Limbourg belgo-neerlandais ou se trouve le Maastrich tien type. et plus specialement а la carriere d'Halembaye 2. GEOGRAPHICAL SITUATION AND LITHO et dans plusieurs localites autour de Beutenaken. Des LOGICAL DESCRIPTION OF STUDIED resultats analytiques sont apportes quant а la distribution SECTIONS ...... 4 verticale d'organismes marqueurs dans les craies situees 2.1. The C.P.L. quarry at Halembaye (Bel- de part et d'autre de cette limite. tant aux plans biostra gian Limburg) ...... 4 tigraphique que paleoecologique 2.1.1. The Vaals Formation ...... 5 La biostratigraphie est assuree par l'expose de la 2.1.2. The Gulpen Formation ...... 5 distribution verticale des principaux marqueurs parmi les 2.1 .2.1 . The Zeven Wegen macrofossiles-Belemnites et autres Cephalopodes - Member ...... 5 ainsi que parmi les microfossiles tels que les Foraminife 2.1.2.2. The Vijlen Member ...... 6 res planctoniques et benthiques. le Nannoplancton et les 2.1 .2.3. The Lixhe Members ...... 6 Dinoflagelles. Les caracteristiques du paleoenvironne 2.1.2.4. The Lanaye Member ...... 6 ment des diverses craies sont deduites de l'etude 2.2. The quarry Habets at Beutenaken (Ne- quantitative de groupes fossiles consideres comme bons therlands Limburg) ...... 6 marqueurs ecologiques, par exemple. les mesofossiles. 2.3. The Bovenste Bosch quarry at Epen les Ostracodes et les Spores-Pollens. Suivant sa valeur (Netherlands Limburg) ...... 7 propre. chacun des groupes permet de definir des zones 2.4. The Borehole КВ 423 at Cadier en Keer biostratigraphiques ou des ecozones. (Netherlands Limburg) ...... 8 Par ailleurs. la proposition de la Sous-Commission 3. - ТНЕ BASE OF ТНЕ MAASTRICHTIAN lnternationale de Stratigraphie du Cretace faisant debu STAGE ...... 9 ter l'etage Maastrichtien avec l'apparition de la Belem nite Belemnella lanceolata est adoptee dans се travail. 3.1. Historical review of the concept of the Maastrichtian stage ...... 9 En tenant compte de cette definition. la craie Ыanche 3.2. The present definition of the base of de Zeven Wegen et а Belemnitel/a mucronata Belemni the Maastrichtian stage ...... 9 tella mucronata "minor" est attribuee au Campanien superieur. la craie de Beutenaken а Ве/етпе//а lanceo 4. WHAT IS ТНЕ MAASTRICHTIAN IN ТНЕ lata inflataet Belemnella "occidentalis" est attribuee а la ТУРЕ REGION ...... 12 partie inferieure du Maastrichtien inferieur tandis que la 4.1. The "type section" of the Maastrichtian 12 craie grise de Vijlen appartient la а Belemnitella junior а 4.2. Correlation of local sections in the partie inferieure du Maastrichtien superieur. De longues Maastricht region ...... 12 periodes d'arret de sedimentation separent les trois unites lithologiques et sont soulignees par des hard 5. - BIOSTRATIGRAPHY : ANALYТICAL RE- grounds. Pourtant il semЫe que des remaniements SU LTS ...... 15 n'aient ete enregistres que sur quelques centimetres а 5.1. Cephalopods : Belemnites ...... 15 un ou deux decimetres la base de chaque unite а 5.1.1. lntroduction...... 15 lithologique. 5.1.2. Historical review ...... 16 Les extensions verticales des differentes especes de 5.1 .3. Description of the material ...... 16 macrofossiles, de Foraminiferes, Nannoplancton. Dino 5.1.4. Stratigraphical observations...... 18 flagelles. Spores-Pollens. mesofossiles et Ostracodes 5.1.5. Definition of Late Cretaceous sont presentees dans une serie de taЫeaux et leurs belemnite zones in Limburg ...... 21 valeurs stratigraphique et ecologique sont discutees. 5.1 .6. Conclusions ...... 22 5.2. Other Cephalopods and other macro- Mots-clefs : Limite stratigraphique, Campanien. Maas fossils ...... 23 trichtien. Biostratigraphie. Faune belemnite, Strato 5.3. Foraminifera ...... 23 type, Pays-Bas, Belgique, Limbourg. 5.3.1. Benthic Foraminifera ...... 23 5.3.2. Planktonic Foraminifera ...... 25 5.4. Nannoplankton ...... 25 5.4.1. Main Ьiostratigraphic results ...... 31 5.4.2. Biozonation ...... 31 BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT з

5.5. Dinoflagellates ...... 32 (1927); Jштzку (1951); VAN DER HEIDE (1954); BERG 5.5.1 . Previous works...... 32 GREN (1964); EL NдGGAR (1966); Sснмю (1967); 5.5.2. Analytical results ...... 32 VILLAIN (1977); ROBASZYNSKI et а/. (Colloque de 5.5.3. Biostratigraphical dinocyst spe- Marseille 1983, in press); B1RKELUND et al. (1984); cies...... 33 et 5.5.4. Remarks ...... 33 ScнuLZ а/. (1984). 5.6. Spores and pollen grains ...... 33 At first sight. the biostratigraphical arguments 5.6.1. Halembaye quarry...... 33 for defining the limits and the subdivisions of the 5.6.2. Beutenaken section...... 37 Maastrichtian stage аге quite different in the 5.6.3. Cadier en Кеег borehole ...... 37 Boreal and in the Tethyan realms. ln brief, in the Boreal realm. the main "traditional" fossil markers. 6. PALAEOECOLOGY AND PALAEOENVI- the most largely used belong to the groups of RONMENT ...... 40 Belemnites and small benthic Foraminifera, whe 6.1. Macrofossils : Belemnites ...... 40 reas in the Tethyan realm. in the absence of these 6.2. Mesofossils ...... 40 groups, planktonic and sometimes large benthic 6.2.1. lntroduction...... 40 Foraminifera аге preferred. Some groups of micro 6.2.2. Remarks оп mesofossil groups 43 fossils аге common in the two realms. such as 6.2.3. Ouantitative distribution ...... 43 Nannoplankton and Dinoflagellates. However. the 6.3. Ostracods...... 43 6.3.1. Historical review ...... 43 vertical distribution of species (paraspecies) be 6.3.2. Palaeoecological value ...... 50 longing to these groups appears insufficiently 6.3.3. Definition of ostracod ecozones 51 correlated with that of the traditional markers in 6.3.4. Species diversity...... 53 the two realms. Consequently. at this time. Nan 6.3.5. Palaeoecological implications .... 53 noplankton and Dinoflagellates could not Ье used 6.4. Spores and pollen grains and organic as markers for defining the Campanian-Maastrich matter ...... 53 tian boundary. 6.4.1. Reworked Spores and pollen As the Maastrichtian was named in the Boreal grains...... 54 6.4.2. Organic matter...... 54 realm, а first step leading to а better understan 6.5. Foraminifera...... 56 ding of what is the Campanian-Maastrichtian 6.5.1. Benthic Foraminifera...... 56 boundary has to Ье made in the Maastricht агеа, 6.5.2. Planktonic Foraminifera and even if. and particularly because. the concept of sea-depth ...... 56 the Maastrichtian stage has much evolved since its 6.6. Nannoplankton and Dinoflagellates .... 56 creation. As а matter of fact, the "type-Maastrich 6.7. Palaeoecological synthesis ...... 57 tian" of DuмoNТ (1849) was defined only оп а 6.7.1. Palaeogeographical influences" 57 lithological base and this was supported later Ьу 6.7.2. Relative water depth...... 57 the lithologic subdivisions Ma-Mb-Mc-Md given 6.7.3. Relative distance of the shore Ьу UHLENBROEK (1905, 1912) and still largely used line ...... 57 for regional works. But, since 1951, the Maastrich 6.7.4. Relative temperature...... 58 tian stage is understood in а wider sense in the 6.7.5. Water energy ...... 58 6.7.6. Substrate...... 58 Boreal realm, following the studies of JELEтzкv 6.7.7. Conclusions ...... 58 (1949. 1951) оп the Belemnites of the chalk in the North European countries. This concept revives 7. CONCLUSIONS...... 59 that of ARKHANGELSKY (1912) and it was implicitly ог 8. REFERENCES ...... 62 explicitly accepted Ьу workers in the northern province. The proposals made during the Creta ceous Stage Boundaries Symposium. held in 1. - INTRODUCTION Copenhagen in October 1983 (81RKELUND et а/., 1984), mark an agreement of а very large majority to place the base of the Maastrichtian stage in the ln the past decades. the boundary between the Boreal realm at the first арреагепсе of Ве/етпе//а Campanian and the Maastrichtian stages was lanceolata. linked to the interpretation of authors of what was lf we follow these proposals, опе сап put considered as the Maastrichtian stage and espe forward the question of what is ог what has cially the base of this stage. The status of the become (in а Ьiostratigraphical sense) the Cam Maastrichtian stage has Ьееп reviewed ог recon panian-Maastrichtian boundary in the Maastricht sidered several times following its creation Ьу агеа. Therefore. the first purpose of this рарег is to DuмoNт in 1849, and more accurately Ьу LERICHE 'present in the most accurate way possiЫe the 4 F. ROBASZYNSКI ЕТ COLL. BCREDP 9 (1985)

vertical distribution of species of the main pa Some of the quarries ог outcrops studied in this laeontological groups occurring in the Campa-· work have Ьееп previously described (completely nian-Maastrichtian chalky facies exposed close to ог partly) Ьу Ruтот (1894); FRдNCKEN (1947); CдLEM the Maastricht locality. Preliminary results of this BERT (1953, 1956). CALEMBERT & MEIJER (1956); study were presented at the "Colloque sur le CдLEMBERT, MEIJER & MONJOIE (1970); HOFKER (1966); Senonien"held in Marseille in October 1983 (see 0EROO (1966); FELDER (1975); ALBERS (1976); VILLAIN RoвдSZYNSKI et а/., 1985). Могеоvег, to explain (1977); Sтяш et а/. (1977); FELDER (1978); FELDER some of the peculiarities of the vertical and lateral etal. (1980). fossil distribution, the palaeoecological conditions of sedimentation of the various chalk facies аге specified Ьу the quantitative study of several good 2.1. ТНЕ "CIMENTS PORTLAND LIEGOIS" (C.P.L.) ecological marker groups. QUARRY АТ HALEMBAYE (BELGIAN LIMBURG)

The C.P.L. quarry is situated оп the left bank of the Meuse river, about 1О km south of Maastricht 2. - GEOGRAPHICAL SIТUATION (Fig. 1 ). From the base to the top, some 90 m of AND LITHOLOGICAL DESCRIPTION calcilutites and calcarenites. more ог less flinty, аге OF STUDIED SECTIONS worked for the fabrication of Portland cement (P.J.F. and F.R.) (Fig. 2).

KS16 borehole GERMANY KS17 Q borehole

N 1 ТНЕ NEТHERLANDS о km

BELGIUM HEERLEN

KUNRADE (!/

С?Ь Qwalem Valkenburg Kunrade Q о 0Nekami

Cadierо en Кееr ф GULPEN КВ 423 borehole . BEUTENAКEN Habets quarry -...... ддСНЕN + + VAALS + Q + \ (11 tJ EPEN + + ++ ++.++ SLENA�EN l:'D +\ + ++ + � + ++ + + + + + + ++ + ++�+ + + +(J + \ + + ++ ++ • ++ + +++ ++ ,.- �+ •• Bovenste Bosch· '+ quarry : + + +++ ++++ FIGURE 1 Location map of quarries and outcrops studied BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 5

"' 1:! :1! 1!! ; а:... э: HALEMBAYE а: а:; "' z1D ;... ffi .. "' о "'w C.P.L. quаггу о... !:; � а: u� � LICHTENBEAG HOAIZON ·---- ·- •• 90 z .. � numb•r of fh• 1&1 flinl 1.-or ,с F с,, .!� z r,r•y flinls ... �1 � sampl•s 1 NIVELLE HOAIZON 80 u • · -HAL.82·13 z ._.., Ьl•с• f/inls а: (1 -HAL.82-18 о .!Е uli� • BOIAS HOAIZON 11'1 -HAL.82-12 .. 70 ,с . � 1- Е Cr3c .. N ,с ...i . t! ! 1&1 -< - .. � :i:: НАLЕМВАVЕ НOAIZON-�(- ·.:,.·:-:::-1-� ! � . Echinocorys I•"•' а: � li :.; ·s ...J 1&1 60 -HAL.82·11 Q: CL .1! •' CL Cr31 :; о LIXHEsWAHLWILLEA HOAIZON - :) u... D .. .! - HAL.82·15 - HAL.82·10 50 � 11' ... i i = 111 с � :1 z - HAL.82-9 1&1 � ...J z ·;. � -, u" > -HAL.82·8 ...J w FROIOМONТ aSLENAKEN HORIZDN - 1,() r: Froidmont - НАL. 82-7 а. h•rd ground 'j .оt z ....J Cr3b Е :! - HAL.82·6 z ::) � ::1:.. 30 ,с (!) � FIGURE 2. - Lithology and sampling CL z - HAL.82·5 ::1: 1 ! 1&1 in the CPL quarry (Ciments Portland ,с А ;, li u ;; 1&1 Liegeois) at Halembaye, Belgium ��!.! з: (GI = glauconite) а: ё.!! 20 - HAL.82-1, 1&1 z g.a 1&1 CL ·� !·� 1&1 :) N . gl•uconitic - HAL.82-, Cr3a ·� ,,,.,� LOEN.ZEVEN WEGEN HOAIZON - 10 - HAL.82·3 ...i.._ � - HAL.82·2 u.. i - - � Cr2 ·8': .. HAL. 82 16 � .!••� - HAL82·1 � 11 1 ; с i G\.

Two formations аге partly exposed in the (see paragraphs 5.1.4. and 5.3.1.). lt consists of Halembaye quarry, the Vaals Formation at the glauconite-bearing silt. with clayey and marly base. overlain Ьу the Gulpen Formation. beds. Weathered sections show а rhythmic suc Remark: "Halembaye" is the spelling used in the cession of hard and soft layers. Belemnites and 1 : 25 ООО topographic map Tongeren-Herderen Pelecypods (mainly Ostrea) аге the only common 34/5-6. 1976 edition, puЬlished Ьу · the lnstitut macrofossils. The upper part of the Vaals Forma Geographique National of Bruxelles. Sometimes tion is absent (due to erosion ог interruption of the the spelling "Hallembaye" is also used, for exam sedimentation). ple in commercial maps and in some past ог recent literature. 2.1.2. The Gulpen Formation

2.1.1. The Vaals Formation This formation is subdivided into six members which аге presented in ascending order. The Vaals Formation. which has а maximum thickness of 150 m in the eastern part of South 2.1.2.1 . The Zeven Wegen МетЬег Limburg, is only some 20 m thick around Halem baye. The outcropping strata in the C.P.L. quarry The member is 29 m thick and consists of belong to the lower part of the Vaals Formation white, fine grained chalk with а few small Ыасk 6 F. ROBASlYNSКI ЕТ COLL. BCREDP 9 (1985) flint nodules. The base of the member is formed follows а bed with randomly distributed flints, Ьу а glauconitic chalk layer of 0.5-0.3 m whereas in the upper part of the member the flints thick = Cr3a of UнLENBROEK (1912). At the top, а are bedded in layers which increase in thickness. well developed hardground occurs, including The thickness of the total member varies between many burrows filled with material introduced from 7.5 m and 10 m. The calcilutitic chalk is extremely younger, overlaying beds ( cf BROMLEY, 1975, and poor in macrofossils. Only fragments of Belemni BROMLEY in FELDER et а/., 1980). Sometimes, the tes and Echinoids аге found. glauconitic layer at the base bears а rich echino derm fauna : Echinocoгys spp., Echinocoгys - The Lixhe 3 Member conicus (AGдss1z), Galeola papillosa (KLEIN), Galeri ln this member flints occur in 15 well-develo tes sulcatoradiatus (GoшFuss) and Micraster co ped layers which сап Ье recognized throughout ranguinum schroederi SтoLLEY. Other main macro the region. About eight metres thick, the calciluti fossils are Pelecypods and Belemnites as Belemni tes аге white to grey and роог in macrofossils. tella mucronata (ScнLOTHEIM) and Belemnitel/a Only in its upper part occur Crinoids and Belemni mucronata "minor" JELEТZKY. tes, normally in the chalk layers without flint

2.1 .2.2. The Vijlen МетЬег 2.1.2.4. The Lanaye МетЬег The thickness and composition of this member ln the C.P.L. quarry the Lanaye Member forms differ from place to place. ln the C.P.L. quarry the the top of the exposed Cretaceous. Only the lower Vijlen Member is about 14.5 m thick and the chalk portion of this member is exposed in the most is grey-white with light grey flints and some northern part of the quarry (from the Nivelle fine-grained glauconite. The chalk is rich in Horizon to flint layer п0 10). The flint layers in the macrofossils. especially Brachiopods (Magas, Te Lanaye Member сап Ье recognized through the rebratulina and Cretirhynchia), Echinoids and whole area. The total member contains 23 flint Belemnites as Belemnitella junior (Nоwдк). The layers and is up to 20 m thick. lt is true calcarenite, thickness of this member increases some kilome white to grey ог yellow. ln the lower part (up to flint tres to the north to more than 50 m and also the layer п0 10), Crinoids and Belemnites аге common glauconite content increases. То the south the macrofossils. ln the upper part (above flint layer thickness decreases to less than 8 m chalk, with по 10), the calcarenite becomes rich in macrofos hardly апу glauconite. sils (Brachiopods, Pelecypods, Crinoids, Echi noids, Bryozoans and Octocorals). ln this part 2.1 .2.3. The Lixhe Members occur also Hemipneustes striatoradiatus (LESKE), Al/opleuron hoffmanni (GRдY). Mosasaurus hoff Based оп the occurrence of flint, three Lixhe manni (MдNTELL) and Mosasaurus lemonnieri Members аге recognized. DoLLO (cf MEIJER, 1984; PLISNIER & COUPATEZ, 1969). - The Lixhe 1 Member ln the Halembaye quarry, the grain size increa lt consists of white to grey calcilutites with ses upwards from the fine-grained and soft chalk irregular dark-grey to Ыасk flints. The base is at the base of the Gulpen Formation into coarse characterized Ьу the first Ыасk flint layer which сап grained calcarenite in the Lanaye Member. Ье followed through the quarry and the surroun ding area. The top of the member is the next Ыасk flint layer (Halembaye 1) which сап Ье followed 2.2. ТНЕ QUARRY НАВЕТS АТ BEUTENAKEN over а large distance. The two flint layers have а (NETHERLANDS LIMBURG) distance of about 8.5 m. The calcilutitic chalk is rich in macrofossils (mainly the same Brachiopods This quarry is ап old abandoned quarry оп the as in the Vijlen Member). The upper part is eastern slope of the valley cut out Ьу the Gulp extremely rich in Echinoids (Echinocorys level). river. lt is the type location of the Beutenaken Belemnites as Belemnitel/a junior аге also com Member (Fig. 3). However, the top of the Beutena mon. ken Member is not exposed in the quarry itself, but - The Lixhe 2 Member some metres higher up in the valley slope. The exposed chalk of the Beutenaken Member is white This consists of white to grey calcilutites with to yellow with some glauconite, increasing at the many irregular dark-grey to Ыасk flints. At the base. The base is а glauconitic chalk. Below the base two well-developed flint layers (Halembaye 1 Beutenaken МеmЬег, the Zeven Wegen МеmЬег and Halembaye 2) occur. Above these two layers consists of white-yellow chalk. At the top, а poorly ВСАЕОР 9 (1985) CAMPANIAN-MAASTR/CHTIAN BOUNDARY NEAR МААSТА/СНТ 7

(VIJLEN МЕМВЕ А ) BEUTENAKEN : quarry Habets ВOVENSTE ВОSСН НORIZON --

z � ВЕUТ.82-1 411: j:: :х: u � ВЕUТ 82-2 � z BEUTENAKEN 15 � � MEMBER � BEUT. 82-3 �� о:: � (fin•ly glauconious � BEUT. 82-1. Ш О:: chalk) �о...J u.. � BEUT. 82-5

SLENAI\EN HORIZON

f- BEUT. 82 -6 FIGURE 3 ZEV EN The sampling in the quarry Habets at WEGEN Beutenaken. Netherlands (GI = glau conite) MEMBER (whit• chalk) f- BEUT. 82-7

! VAALS FORMATION

developed hardground occurs. The higher part of Ga/eola papillosa KLEIN) and internal moulds of the chalk contains nearly по glauconite. whereas heteromorph Ammonites. The chalk is capped Ьу in the lower part the glauconite content increases ап indistinct hardground. the -Slenaken - hard and forms а glauconitic chalk. Macrofossils аге ground. гаге. but occasionally Belemnites and hetero The overlying yellow-grey. glauconitic chalk of morph Ammonites аге found. At the base of the the Beutenaken Member is also vегу fine-grained quarry some metres of the middle Vaals Formation and роог in macrofossils. except for Belemnites in аге exposed. consisting of а sandy silt with some the basal. vегу glauconitic layer оп top of the marly layers. Slenaken hardground. The top of the Beutenaken Member is also marked Ьу а hardground : the Bovenste Bosch hardground. This hardground сап Ье rich in (partly reworked) fossils amongst which 2.3. ТНЕ BOVENSTE BOSCH QUARRY АТ EPEN there аге many Belemnites. (NETHERLANDS LIMBURG) The level is overlain Ьу а basal conglomerate. consisting of rounded fragmented Belemnites and phosphatized fossils, limestone, quartz and quart This is а small. abandoned and decayed quarry zite реЬЫеs. These аге embedded in. а glauconitic оп the southern slope of the Geul Valley at Ереп chalk matrix. Because of the abundance of belem (Fig. 4). The Cretaceous rocks аге largely covered nite fragments. this basal conglomerate is known Ьу slope debris. The section shows the upper as the "Belemnite graveyard". Upwards. this layer portion of the Zeven Wegen Member. the Beute passes into а yellow-grey, fine-grained, glauconitic naken Member and the basal part of the Vijlen chalk with а wealth of macrofossils : Belemnites. Member. А borehole in the quarry demonstrated Echinoids such as Echinocorys limburgicus (l.Aм that the Zeven Wegen Member is about 1 О m BERT), Echinogalerus belgicus (l.АмвЕRт). Cardiaster thick. and is overlying marly sands of the Vaals granulosus (GoшFUss). Galerites su/catoradiatus Formation. (GoшFUss). Brachiopods such as Terebratulidae. The poorly fossiliferous. vегу fine-grained. Rhynchonellidae. and Craniidae. bivalve frag whitish-yellow chalk of the Zeven Wegen Member ments. and Cephalopods : Nautiloidea. Ammonoi has yielded а few echinoids (Echinocorys sp., •dea

10 F. ROBASZYNSKI ET COLL BCREDP 9 (1985)

� d' OMALIU S DUMONT d'ORB. �- � I 1808 1828 1832 1843 l&J 0 a:... p. 153 p. 569, 573 p.294 - 296 p.403 0:: l&J a: m 0:: l&J m l&J � z � 0 La. l&J_. _.l&J _. 0 4( l&J ]: 5 u �

- VROENHOVEN HORIZON -1r.,,,._,..,.,..,..,,7'.,...t z N 0 MEERSSEN I� ...ENCi Md MEMBER UBAGHS M 1887 Sid•rolilH V OrbiloidH L Sph. bincth -CASTER HORIZON ----t'1P"'n7?m"1 Rudi,t Calcaire tuffeau calcaire H•mipn. grossi er de t- K Mc NEKUM M. _ � de MHstricht de I - LAU MONT HORIZON- - - , - , .. _, • f l u Maestr. flint, o: I EMAEL M. Maistricht I- - ROMONT11JSCH HORIZON- -- � (f) Mb :c SCHIEPERSBERG. M. ... GRONSVELD M. u u � H , ' VALKEN BURG M. � . -- North � � -@@�----t-LICHTENBERG HORIZON --t-i,-.--c::::.. =::>--1 \ :'\ /\ /\\,,/\ ! etag e inf lll .. \.! \.,i ...� • LANAYE gr•y ��-=- V V I : bancs cl .!iii _,.._.. u cl F Cr4 :!"ii MEMBER flint, ....-,. cont inus :""":::.= de silex � ueOI gris --t--�---NIVELLE HORIZON- .. ___ • C black ,'\ /\ I::�:_..�-� ...... ,/ I I I/\ \ ,,\ LIXHE 3 M. flint, a: \/ \,'\ \V ,' , \ UJ z -:: - BOIRS HORIZON----;/\:<1 � " Q. 0 :.• :, .: ··� - Q. E Cr3c .2' LIXHE 2 M. ·=-· .. : .. -:-:-:-· � craie craie 11 ,-- HALEMBAYE HORIZON -1:;.-.r------Echinoc. ·� LIXHE 1 M. Ill u blanche C 3 __ rc__ ._.Y_--;,-- LIXHE:WAHL. HORIZON - ·:::::_: CJ).. D �- � • 11 VIJLEN MEMBER C "ii.!!! � ...... �L. z u OI crail" -� -� � � -- FROIDMONT: SL. HORIZON -1"'71'°"'7:!'7)71·- •·• -- ... "'Cl iii w ·1 • 'l � a.. �... = � ...J Cr3b z . I u .. ZEVEN WEGEN L. � :) I .!!! - � C!:> A MEMBER I : u C 2 I -� � • 0 C ffi I C II K:r3a -� 1 • I : �-+---+-�.:;.;..;;.,;;;;i1---....-t LOEN :ZEV. WEG. HORIZ. -- �.':,'.:.�'.�,' �. a: (f) ..,. . ., .. , ... . .! �:::, -..0 Crl II L j L. :::: � i � YYff ;[Jj ... � FIGURE 6 Historical evolution of the concept of Maastrichtian stage in the Maastricht area (o·ORB. = o·ORBIGNY. B1NCKH VAN BINCKHORST, CAL = CALEMBERT) BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 11

DUMONT BINCKH STARING DEWALOUE geol. map. RUT OT HAUG UHLENBROEK CAL SCHMID SCHULZ and 1849 1859 1860 1868 1892-1929 1894 1911 1912 1956 1967 SCHMID p.360-361 p.24 p.317-34 2 p.154 (Belgium) tabl.p.185 p.1170 p.49-52 p.131. p.473 1983 140

z Danien z - - ············ -@ -icht 0 ,t., � grey I Cr4 flints ·1OI a: Ill ..; c - - u I.LI -·- - m - ., 0 _.,.... .&. tijger I.LI Cl I- ·- krijt Assise u Crlc Gulpen - -, 3

CJJ ("') m:JJ � 0 UJ _, KS16 KS17 KUI\RADE LAHAYE ENCi !£KAMI VAl..tael.RG WAL EM

ROMONTSBOSCH HORIZON 1-:::-_, l•:�e-_•I P.'� Ii ("') � � -=- � i _±- z Zlw )> UJ j -=- z a: i : �� (1c,,Tf:,.8El/r; i::, a.I! � ·= CJ) I I -i I�;:; I :;]J ·� I n _.-� I -i :1- - )> �11°"·-Fr.cil - CAOIER .n K z a:, ·.to BEUTENAIIEN 0 s,��+s,, C +�'i'E 11:; : � z ::, �(lp BB. . l!EUT. LEGEND 0 & lit!; MEie ·,: .. ,-·. � (OEN :·:.;.7'�_: :JJ C "' -I 11DR1zo,. u -< ,c:( .,6I}f: .:/.·:·.;·:.: Ochalk z -i � :�(T.+) 8f0i'.�: m 'I ! � z I \CJ(\ :.£.t-. � Limestone :JJ UJ :-..-�-r .. �;s1& ::7:-:-;-:· � ::,":"-:".;·.· n1�,1 ::;:·.-:,,:·. � Marl,marly ,c:( ii&. VAALS ·:..!.:':::�.:- t ,c:( : CJ) -i :I /t+. :JJ FORMATION ::,:,-:,.;:. CJ] Slit.sand :��(··,�.;·.:::-:· n i NL··········(. :.�::;·.:·. I /?7-f:/ z.�r.:::;:·:.-,,:.: �:.;-�f-:":' ;:,':"":"':;(.", -i ·· -� :;':"':":;:::. cill:}{2 � Pebbles �unr. ()· {8\/ .:;�;�::: :;·.::;·::: Flint �c�:\k. ::,":"':-:.·;:.: E:J LI :7:'::;::: -:··· D -. ••• � .. � Fossil grit �J ....•""• ...... :.�'.;.. \ II L ...... _. � '-. / B �IOlim W Glauconite

FIGURE 8 Correlation chart of local lithostratigraphical sections for the Campanian-Maastrichtian in South-Limburg c..., 14 F. ROBASZVNSKI ET COLL. BCREDP 9 (1985) lands Graben) to the north-east and the Ardennp Rhenish Massif to the south-east (Fig. 7). The most important gap occurs around the Campanian \!! ::: z: Maastricht Formation seem to be more completely developed. At the same time, the critical interval - comprising the Campanian- z Maastrichtian boundary - is absent in the Halem-

Several erosion horizons or hardgrounds within area may be best explained by accepting rotational the Gulpen Formation indicate repeated interrup movements of the basin floor parallel to the tion of the sedimentation and even erosion during NW-SE striking faults of the Rur Valley Graben. the latest Campanian until the Upper Maastrich The rate of subsidence was highest in the north tian. Lower Maastrichtian deposits are restricted to east (Walem-Valkenburg and Campine areas) the Beutenaken Member of limited lateral exten during the deposition of the Vaals and Maastricht sion and characterized by glauconite and belem Formations, and highest to the south-west (Ha nite guards of Lower Maastrichtian age. The lo lembaye area) during the deposition of the Gulpen wermost Upper Maastrichtian deposits within the Formation. This overall pattern has been complica Gulpen Formation (Vijlen to Lixhe-3 Members) are ted by the fact that this basin floor was broken up overstepped towards the north-east by the top into smaller tectonic units showing differential most Gulpen sediments of the Lanaye Member. rates of subsidence (cakewalk movements). The sediments of the Gulpen Formation consist Thus, in such a depository context. it appears of marine. very fine-grained chalk (calcilutites to that the Maastrichtian cannot be defined on one calcisiltites) with an upward increasing amount of section only, the thicknesses and lateral facies chert (usually concentrated in widespread beds variations being relatively too important. In this which can be traced throughout the area). Bivalves way, to seize the connections between the diffe and belemnite guards abound in some layers. The rent lithological units, it is more realistic to use a sediment and the fossil assemblages suggest that type region to understand the Maastrichtian of deposition occurred in an open marine environ Limburg (the Netherlands and Belgium). ment that was slightly deeper than that of the A different solution might be found in accep Vaals Formation. ting that the upper portion of the Vaals Formation A renewed period of erosion and/or non-depo (upper A' Foraminifera Zone) and the lower portion sition is represented by the Lichtenberg Horizon of the Maastricht Formation (ecozone 4 according separating the Maastricht Formation from the to mesofossils) might be the northern, lateral underlying Gulpen Formation (in the south-west) equivalent of the Gulpen Formation. In that case, or Vaals Formation (to the north-east). The oldest the Campanian-Maastrichtian boundary might be deposits of the Maastricht Formation are found in, recognized some day also in a possibly nearshore respectively, the Campine area (KS16-KS17) and environment where abundant belemnite guards around Valkenburg-Walem. From Valkenburg to seem to occur. This possibility will be dealt with in Lanaye, the lower Maastricht Formation gradually another paper by FELDER et al. in the Professional oversteps always younger sediments of the La Papers of the Geological Survey of Belgium. In that naye Member of the Gulpen Formation. case, the sedimentary gaps would be much smal ler than accepted here and in the previous literature. The oldest (marly) deposits of the Maastricht Formation bear an upward decreasing admixture of glauconite and silt/sand. Higher upwards, a sequence of alternating hard/soft chalk occurs with 5. - BIOSTRATIGRAPHY: locally shale and coal pebbles derived from Upper ANALYTICAL RESULTS Carboniferous rocks which presumably had been exposed to erosion somewhere to the north-east. This sequence may be slightly diachronous and is 5.1. CEPHALOPODS: BELEMNITES (L.A. VDT.) replaced towards the south-west by fine-grained to coarse-grained chalk (calcilutites to calcareni tes) with flint layers. A number of hardgrounds in 5.1 .1 . Introduction the higher portion of the Maastricht Formation In Limburg, the Netherlands and Belgium, suggests a repeated interruption of the sedimenta belemnite guards can be the most usable macro tion. Also the boundary between the Maastricht fossils for biostratigraphical purposes, because Formation and the Early Tertiary (Paleocene) they are found more frequently and are less Houthem Formation is marked by a hardground facies-bound than other macrofossils. Therefore, a (Vroenhoven hardground). The rather diverse fossil good knowledge of the stratigraphical range of the assemblages of the Maastricht Formation are several belemnite species is desirable. The more frequently shallow marine facies. so as the boundaries between the stages and The rather complex depositional history of the substages of the upper part of the Cretaceous in Late Cretaceous sediments in the South-Limburg the Boreal realm are largely based on Belemnites. F. ROBASlYNSKI ET COLL. BCREDP 9 (1985)

The following belemnite species are found Ln nella lanceolata inflata preserved in local depres the Upper Cretaceous of Limburg : Gonioteuthis sions. quadrata (BLAINVILLE). Belemnitella mucronata Note : The locality Beutenaken is taken in a wider sense (ScHLOTHEIM). Belemnitella mucronata m,nor than only the Habets quarrynear Beutenaken. because of the poorness of the available material. With the locality sensu JELETZKY. Belemnitel/a junior NOWAK. Belem "Beutenaken" is meant in this paper the area around (ARKHANGELSKY). nella lanceolata inflata Belemnella Beutenaken with the localities as shown in the map "occidentalis "sensu B1RKELUND. Belemnella casimi (Fig. 10). rovensis (SKOLOZDROWNA). All these belemnite spe cies are found in the localities of Halembaye and Beutenaken. with the exception in both localities 5.1.2. Historical review of Belemnella casimirovensis. In these localities the Campanian-Maastrichtian boundary is clearly In the 19th century and a large part of the 20th marked at the base of the Maastrichtian layers by century. Limburg Belemnites were commonly re a rich belemnite bed related to a gap of sedimen ferred to as "Actinocamax quadratus" for the tation. Lower Campanian forms and "Belemnites mucro natus" for all other Belemnites (e.g. 81NCKHORST. For the Upper Cretaceous sediments of the 1861; 80SOUET. 1860; SCHLUTER. 1876; HOLZAPFEL, "Ciments Portland Liegeois" quarry (C.P.L.) at 1888; VAN DER WEIJDEN, 1943). This situation conti Halembaye. we can recognize the following be nued to exist until some workers on Belemnites lemnite zones : the Gonioteuthis quadrata Zone. reviewed the older literature and made more the Belemnitella mucronata Zone and the Belemni differentiated lists (JELETZKY, 1951 ). Real fieldwork tel/a mucronata "minor" Zone of the Campanian; was done for the first time by SCHMID (1959) who and the Belemnitella junior Zone of the Maastrich made the first useful biozonation in Limburg based tian. on Belemnites. After the detailed lithostratigraphi In the Upper Cretaceous sediments of Beute cal studies of FELDER (1975 a. 1975 b) it was naken five belemnite zones can be recognized : possible for VAN DER TuuK & BoR (1980) to make a the Belemnitella mucronata Zone and the Belemni more detailed lithostratigraphically correlated bio tella mucronata "minor" Zone of the Campanian; zonation, mainly based on SCHMID (1959). the Belemnella lanceolata Zone. the Belemnella Zone and the "occidentalis" Belemnitella junior 5.1 .3. Description of the material Zone of the Maastrichtian. The belemnite guards of Belemnella lanceolata inflata and Belemnel/a · Nowadays, belemnite systematic is still unsatis "occidentalis" are very abundant at the top of the factory. In order to avoid unnecessary confusion. a Beutenaken Member. short description of the material is given. However. It is striking that the Belemnella lanceolata Zone one must not consider the present paper as a is extant only in Beutenaken and not in Halem complete systematical work. For that. the following baye. Here the Belemnella /anceolata Zone is papers are suggested : 81RKELUND ( 1957); CHRISTEN marked only above the Froidmont hardground by SEN (1975); JELETZKY (1949. 1951); SCHULZ (1979). the presence of rare. reworked guards of Be/em- Material that was more or less badly worn is herein

,----,tkm \ \ ;!�:;:L OWahlw.. r O j \ REPUBLIC Plalt•bosch t" ••• ••••• "'\ .... i BELGIUM / '••••• r•' THE NETHERLAMJS < ...... \• ._. M.U.STRICHT i. (••• 0Kosbff9 \ : FIGURE 10 J �&bnludl V • �•n•rbosch Map of localites studied in the Beute 0 : ••• : •••••• S.U.t naken region for their cephalopod �-bop 0 OZ.wnW.O•n content

OCott-n �lenlbosch

OBov.nslif Bosch �011m K�rbosc:ho BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 17 considered to be reworked. Guards that are refer Remarks : The length is the distance between the red to as in situ were found in such a good state apex and the protoconch. There is a pseudoalveo that they are considered to be originally embed lus when the material around the alveolus is not ded. Parts of guards that could not be determined completely calcified, and thus not preserved. because of their fragmental character were not used in this study. The number of retained speci Genus : Belemnitella o·ORBIGNY, 1840 mens is roughly indicated in the stratigraphical tables by the terms : rare ( < 3 specimens), pre Belemnitella mucronata (LINK, 1807) sent (3 - 10 specimens), common (11 - 25 speci (Synonym: NowAK, mens) and abundant ( > 25 specimens). Belemnitella mucronata senior 1913; see CHRISTENSEN et al., 1975) The Belemnites were placed at my disposal by Plate 1, fig. 2a-2b and 3a-3b the Museum of Natural History at Maastricht (collection W.M. Felder) and the Teylers Museum A large guard with a blunt apex on which a well at Haarlem (collection of the author). Belemnite definable mucro is present. Cylindrical or slightly terminology is shown in Fig. 11. lanceolate in ventral view and highly conical in lateral view. Ventrally flattened. The average length Order: Decapoda LEACH, 1818 of adult specimens is about 80 mm. The dorsoven Family: Belemnitidae o·ORBIGNY, 1845 tral diameter- length ratio has an average of 0.28. The alveolar angle is about 20° and the fissure Genus: BAYLE, 1878 Gonioteuthis angle between the bottom of the ventral fissure ° Gonioteuthis quadrata ( BLAINVILLE, 1827) and the wall of the alveolus varies between 5 and ° Plate 1, fig. 1a-1b 50 . The average Schatzky distance is 7 mm. The surface of the guard is marked with longitudinal depressions. double furrows and some longitudi A slender guard with a blunt apex on which a nal striation and vascular imprints. Belemnitella short mucro is present. Slightly lanceolate in mucronata is larger and more conical in lateral ventral view, highly conical in lateral view. The view than Belemnitella mucronata "minor". The average length is 60 mm. The average dorsoventral vascular imprints are better developed than at diameter-length ratio is 0.19. The depth of the Belemnitella mucronata "minor". pseudoalveolus is 10 mm. A short ventral fissure is Belemnitella mucronata "minor" sensu JELETZKY. present. The surface of the guard is marked with 1949; and sensu BIRKELUND, 1957 longitudinal depressions, double furrows and vascular imprints. Almost the complete surface is Plate 2. fig. 1a-1 b and 2a-2b covered with transverse. corrugated granules. Characteristic of this species is the subrhomboidal A rather large guard with a blunt apex. on appearance of the pseudoalveolus in anterior which a hardly definable mucro is present. Slightly view. lanceolate in ventral view, slightly conical, subcy lindrical or lanceolate in lateral view. The average length of adult specimens is 64 mm. The dorso ventral diameter-length ratio has an average of 0.24. The alveolar angle is about 20° and the fissure angle varies between 15° and 90°. The average Schatzky distance is 8.4 mm, but never less than 5 mm. The surface of the guard is marked with longitudinal depressions. double furrows and some longitudinal striae and vascular imprints. Belemnitella mucronata "minor" is thicker, less conical and the surface is more smooth than in Belemnitel/a junior NowAK. Remarks: The described form was referred to as "Belemnitel/a /anger by VAN DER TUUK ( in ROBAS ZYNSKI et al., 1985), which was considered to be � j synonymous with Belemnitella mucronata "minor" FIGURE 11 JELETZKY. The species Belemnitella langei is nowa Morphological features of belemnite guards 'days generally considered to be different from 18 F. ROBASZYNSKI ET COLL BCREDP 9 (1985)

Belemnitella mucronata "minor", and has only Mostly rather slender guard with a well defina been found in Kronsmoor (Germany) and in th·e ble mucro. Highly lanceolate in ventral view, Soviet Union (CHRISTENSEN, pers. comm.). subcylindrical or conical in lateral view. The ave rage length of adult specimens is 51 mm. The Belemnitella junior NowAK, 1913 dorsoventral diameter-length ratio has an average Plate 3, fig. 2a-2b and 3a-3b of 0.22. Juvenile specimens are much more slen der. The alveolar angle is about 17° and the fissure ° ° A large guard with a short mucro. Slightly angle varies between 10 and 40 . The Schatzky lanceolate in ventral view and conical in lateral distance varies between O and 3 mm. The surface view. The length of adult specimens can reach is marked with fine vascular imprints. Belemnella 135 mm. The dorsoventral diameter-length ratio "occidentalis" has a thicker and less lanceolate has an average of 0.20. The alveolar angle is about guard than Belemnella lanceolata (ScHLOT.HEIM, 23° and the fissure angle varies between 17° and 1813) and the bottom of the ventral fissure is less 43°. The average Schatzky distance is 7.5 mm. The sinuous than that of Belemnella lanceolata. surface of the guard has a wrinkled appearance, Remark: The studied material is unfortunately not caused by dense vascular imprints and longitudi well enough preserved to make a more precise nal striae. determination possible. It is therefore very possi ble that we are dealing with the forms Belemnella Genus : Belemnella NOWAK, 1913 obtusa SCHULZ or Belemnella sumensis JELETZKY as described by SCHULZ (1979). Belemnella lanceolata inflata (ARKHANGELSKY, 1912) 5.1.4. Stratigraphical observations (Synonym : Belemnella aft. lanceolata ScHLOTHEIM, 1813. sensu BIRKELUND, 1957, tab. 3, fig. 4). The stratigraphical distribution of the below mentioned belemnite guards in the localities of Plate 2, fig. 3a-3b Halembaye and Beutenaken is given in Fig. 12 and Fig. 13. Gonioteuthis quadrata (of the Lower Cam A very slender guard with a blunt apex, on panian) occurs in situ in the Vaals Formation at the which a hardly definable mucro is present. Highly C.P.L. quarry at Halembaye and is found in the lanceolate in ventral view and slighly lanceolate or upper part of this formation more frequently. In the subcylindrical in lateral view. Ventrally flattened. basal conglomerate or glauconitic chalk of the The average length of adult specimens is 70 mm. Gulpen Formation, numerous reworked guards of The dorsoventral diameter-length ratio has an Gonioteuthis quadrata can be found. Belemnitella average of 0.16. Juvenile specimens are much mucronata occurs in situ in the whole Zeven more slender. The alveolar angle is about 14° and Wegen Member at Halembaye and in the basal the fissure angle varies between 10° and 80°. The conglomerate of the Beutenaken Member at Schatzky distance varies between O and 2.4 mm. Beutenaken. Belemnitella mucronata "minor" oc The surface is marked with hardly visible vascular curs in situ in the upper part of the Zeven Wegen imprints. Belemnella lanceolata inflata is more Member at Halembaye and Beutenaken and is slender and more lanceolate than Belemnella found reworked at the base of the Beutenaken "occidentalis" sensu 81RKELUND, 1957, and has a Member at Beutenaken. Belemnitella junior occurs more sinuous bottom on the ventral fissure. in situ in the upper part of the Gulpen Formation Remarks: The described form was named "Be (Vijlen Member up to the Lanaye Member) at lemnella lanceolata" by VAN DER TuuK (in RosAs Halembaye and in the Vijlen Member at Beutena Belemnel/a lanceolata inflata in situ ZYNSKI et al., 1985), which was a general determina ken. occurs in tion of the more slender forms of Belemnel/ain the the Beutenaken Member at Beutenaken and is Beutenake Member and at the very base of the abundant in its upper part. Reworked guards can Vijlen Member. A more precise determination by be found in the basal conglomerate of the Vijlen naming these forms Belemnella inflata was propo Member at Beutenaken and at the base of the sed by CHRISTENSEN (pers. comm.). As both Belem Vijlen Member at Halembaye. nel/a lanceolata and Belemnel/a lanceolata inflata It is pointed out here that SCHULZ & SCHMID occur in the lower Lower Maastrichtian, there are (1983) describe the finding of Belemnel/a cimbrica no stratigraphical consequences for this paper. B1RKELUND at the base of the Vijlen Member in Halembaye. The present author was not able to Belemnella "occidentalis" sensu B1RKELUND, 1957 incorporate this material in this paper on a short Plate 3, fig. 1 a-1b notice. (l)< � UPPER CAMPANIAN UPPER MAASTRICHTIAN Stag.s c=;· HOFKER 's zon.s (1966) � 0 C EVEN Member Member I LIXHE 1M. :r Formal lithotyp.s(FELDER,1975) a. > ,- Metric scale �- m m§.; :!: , CD (") C ...I I• .• . J_.. � m 0s· ::::,a CJ)ci -O Ql CD ra,] Goniofpufhis quadrata (BLAINVILLE, 1827) ::::, (l) a.CD 8f'IPmnitPlla mucronata (SCHLOTHEIM, 1813) mCJ CD 3 ·----- BPIPmnifPlla mucronata "minor "UELETZKY,1951) r Q)-, -::::,· ::c- BPIPmnPlla lancPolata inflata(ARKHANGELSKY, 1912) m (") (l) J--C/1... ::0- ·J 8PIPmnPlla "occidPntalis" sensu BIRKELUND,1957 � 0 Q) BPIPmnif Piia junior NOWAK , 1913 z "C::::, a. - -- ..... g_ - m CJ) 0 � CD ' � i' N ClJ (/) -· 5- N � 0 Gl N N N ii" 0 Ill 0 ..,n "' 3 0 c· 3 0 n, (/) (l) :, a. :, :, 0 = g s· 3 :::, z z - r Q) -, "' :,1- Ill ID O C 2. n, -t rn a. ;: c5· "' Ill .., ('I � Q. Ul ITI 3:: n � =� i coa. (l) "C ; ;- ji;' a.J Q) � (") 0 Scaphifps hippocrPpis (DEK AY) (") "C T1 n 0 O Q --o-- EufrPphocPras dPprPssus (BINCKHORST) i3._ a. C m -· CJ) :D --0-- Epicyma tocPras vaa lsPnsis (BINCKHORST) ::::, -· m CO•J ...... a. --o-- Acanthoscaphiff'S tridPns ( KNER) }l> ... o ... N ---o--- ..... 0-::::f" ------HoploscaphifPs constricfus fpnuisfriatus ( KNER) o ::0 ---o--- Hoploscaphiff'S constrictus constrictus ( SOWERBY) "'lJm �.c .., - bI m - W"O - .., Ill � ---o--- e wlll :::: 8 N CT Pachydiscus sp. Q::;(J C:::: Q) �o UI-,"' 3 -UI C t N I I ---0--- Conchorhynchus iimburgicus V. � [ �UI "O UIed ID UI 3 UI:, D. TUUK� �� C :=,· i "' Ill 0 "O Cl. � 0 i ;!. "'Ill "' ---0--- Rhyncolitus minimus BINCKHORST ..... n S: :r i· 0 i :, � a. Cl. u,r�-0 "'. 0 • Q) Q) ... ::::, I Echinocorys gr. conicus (AGASSIZ ) a. Q) Echinocorys gibbus (LAMARCK) -. CD �m :::i 3 MicrastPr schroPdPri STOLLEY �g n er mo I r» Q) Catopygus gr. fpnf'sfratus AGASSIZ Cl!< Car diastPr gr. granulosus ( GOLDFUSS) :Dm �� z en -t Echinocorys gr. limburgicus LAMBERT _::c,g 0 C1) J Echinocorys conoidf'US (GOLDFUSS) iii- o -. CD o Qi a. IB u, }i,� CJ CD Magas pumilus SOWERBY ,- l!: ::;(J -..Jcrr l> =�·oo ... Magas sp. 8 a· .,______.,__ ------�:c.., n TPrf'bratuiina gracilis (SCHLOTHEIM) Cl)� :::c ::::, _.,.. :, ....rania------ignabPrgf'nsis RETZIUS ID '° Q S, "'lJ Thf'cidPa papillata (SCHLOTHEIM) - CJ) !!!.o- o 0 TrigonosPmus pPCtiniformis SCHLOTHEIM 0 3 CD ; (/) 20 F. ROBASZYNSKI ET COLL. BCREDP 9 (1985)

UPPER LOWER stao.s UPPER MAASTRICHTIAN CAMPANIAN MAASTRICHT

811 zones . Bit. Bin. Bin. "'minor" lanc.intl "occ'. Bit. junior

me,mbe,rs ZEVEN WEGEN BEUTENAKEN VIJLEN I LANAYE �. 811. mucronata ------:---- : Mechelen

811.mucronala ------:-- 1 Grindgroeve i u inor" -- -- B t. m cronata "m � : Plattebosch hg OY Bit. mucronata ------·------�-:n• Blt.mucronata ·'minor·· ------Bovenste Bosch 1 n lat --- -- · ::� ·� ;�:�: i :'.. � _ _ : _ ::_ : : Epen o a i -- _ �= -- - - :-�------Bit. junior • - - - -· ------' - -

Bit. junior ------Kos berg

Zeven Wegen

junior

Bit junior ------Kerperbosch Ka steel Bin. lanceotata inflala ------Altembrouck

I Bin. lanc•olata inllata -----.- ..-. ---• --.-- - - -. Vijlenerbosch Bit. junior ----···----. -- - - -·-· --- -. -- --... -- .:

Bln. lanceoolata inflata Hoeve Bellet

Bin. lanc•olata inflata FIGURE 13 B In ... occ i�n t aliS.. ---.- --.--. -- -. ------.. -.. ... Malenbosch Vertical distribution of Belemnites Bit.junior ------·------_ in the Beutenaken region ,--, Bit. junior ------{-- : Cottessen '------1 r---, Bit.junior ----t---: '-----' Mamelis

Bit. junior Wahl wilier

� r•work•d b•l•rnnilK - abundant , 25 sp•cim•ns Bit: B•l•rnnit•lla 11-25 spec. Bin: B•l•rnn•lla prn•nt 3 -10sp•c. ho: hardoround rar• < 3 sp•c- OY : "ora.,.yard"

Belemnella "occidenta/is" occurs reworked According to CHRISTENSEN (1975). the Central only in the upper part of the Beutenaken Member European Subprovince was characterized by at Beutenaken and at the base of the Vijlen members of the evolutionary lineage during the Member at Beutenaken and several other locali Santonian and Lower Campanian : Gonioteuthis ties. westfalica, G. westfalicagranulata, G. granulata, G. A belemnite zonation for the Upper Cretaceous granulataquadrata, G. quadrata quadrata and G. of Limburg has been provisionally established by quadrata gracilis. In the Upper Campanian the SCHMID (1959) and VAN DER TuuK & BOA (1980). genus Belemnitella. represented by Belemnitella Although the Cretaceous sections of Limburg are mucronata and Belemnitella mucronata "minor", far from continuous. in the present paper a further expanded its distribution area from the Central attempt is made to establish a biozonation based Russian Subprovince to cover the whole North on belemnite guards. A European belemnite zona European Subprovince. At the transition from the tion has been composed. among others. by Campanian to the Maastrichtian. the genus Be JELETZKY (1951 ), 81RKELUND (1957), CHRISTENSEN (1975) lemnella appears. early forms only in the Central and SCHULZ et al. (1983) as shown in Fig. 14. Russian Subprovince. Lower Maastrichtian forms BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 21

Belemnite Zones Belemnite Zones in NW Europe in Limburg

UPPER Belemnella casimirovensis Belemnella casimirovensis MAASTRICHTIAN Belemnitella junior Belemnitella junior

Belemnella fastigata Belemnella cimbrica ___ ? __Be lemnella_cimbrica___ ? ____ _ LOWER Belemnella sumensis 1 B. "occidentalis" MAASTRICHTIAN Belemnella obtusa sensu BIRI

Belemnitella "langei" UPPER Belemnitella mucronata "minor" Belemnitella mucronata "minor" CAMPAN IAN Belemnitella mucronata ___ Belemnitella_mucronata______

Gonioteuthis quadrata gracilis LOWER /B. mucronata CAMPAN IAN Gonioteuthis quadrata gracilis Gonioteuthis quadrata quadrata Gonioteuthis quadrata Gonioteuthis granulataquadrata

FIGURE 14 Belemnite zones in Limburg compared to belemnite zones of NW Europe (according to JELETZKY. 1951 ; B1RKELUND. 1957; CHRISTENSEN, 1975; SCHULZ et al., 1983) as Belemnella lanceo/ata inflata and Belemnella Lithostratigraphical correlation : Gulpen Forma "occidentalis" are known from most parts of the tion. lower part of the Zeven Wegen Member. North European Subprovince. The Upper Maas Age : Upper Campanian (lower part). trichtian is characterized by Belemnitella junior and Belemnella casimirovensis. The latter is confined Belemnitella mucronata "minor" Taxon-range to the upper part of this substage. zone Definition : Interval from the first to the last occurrence of Belemnitella mucronata "minor". 5.1 .5. Definition of Late Cretaceous belemnite Author: JELETZKY (1951 ). zones in Limburg (see also VAN DER TuuK & BoR. 1980) Lithostratigraphical correlation : Gulpen Forma tion. upper part of the Zeven Wegen Member. Gonioteuthis quadrata Taxon-range-zone Age : Upper Campanian (partly upper part). Definition : Interval from the first to the last Belemnella lanceolata Interval-zone occurrence of Gonioteuthis quadrata. Definition : Interval between the first occur Authors: SCHMID (1957); ERNST (1964). rence of Belemnella lanceolata and the first occur Lithostratigraphical correlation : Vaals Forma rence of Belemnella "occidentalis". In Limburg. tion. this zone is marked by the presence of Belemnella Age : Lower Campanian. lanceolata inflata. Lithostratigraphical correlation : Gulpen Forma Interval-zone Belemnitella mucronata tion. Beutenaken Member. Definition : Interval between the first occur Age : Lower Maastrichtian (lower part). rence of Belemnitel/a mucronata and the first occurrence of Belemnitella mucronata "minor". Belemnella "occidentalis" Interval-zone Author: JELETZKY (1948). Definition : Interval between the first appea- 22 F. ROBASZYNSKI ET COLL. BCREDP 9 (1985) ranee of Belemnella "occidentalis" and the first more strongly reduced at Halembaye than it is at appearance of Belemnella cimbrica. Beutenaken. The absence of almost all of the Remark : in the Beutenaken Member. this zone Lower Maastrichtian at Halembaye is the reason is represented only by reworked material. why the type-Maastrichtian area (Netherlands and Belgian Limburg) is not favourable to constitute a Lithostratigraphical correlation : Gulpen Forma reference for layers below the Vijlen Member. Only tion. upper part of the Beutenaken Member. the Beutenaken Member belongs certainly to the Age : Lower Maastrichtian (lower part) to Upper Lower Maastrichtian. Both in Halembaye and in Maastrichtian (lower part). Beutenaken the whole Zeven Wegen Member is characterized by the occurrence of well-preserved Belemnitella junior Partial-range-zone guards of the Upper Campanian belemnite spe Definition : Interval from the first occurrence of cies Belemnitella mucronata and Belemnitella Belemnitella junior s.l. to the first occurrence of mucronata "minor". The Zeven Wegen Member is Be/emne//a casimirovensis. therefore considered to be Upper Campanian. Both in Halembaye and Beutenaken a hardground Author: JELETZKY (1951 ). is present at the top of the Zeven Wegen Member. Lithostratigraphical correlation : Gulpen Forma This hardground (Froidmont hardground) contains tion. Vijlen Member up to the Lanaye Member. guards of Belemnitella mucronata and Be/emni and the Maastricht Formation. except for the tella mucronata "minor". that show clear signs of uppermost part of the Meerssen Member. post-mortem transport. It is not clear whether Age : Upper Maastrichtian (lower part). these guards are genuinely reworked or if abrasion is the result of deposition in a condensed se Belemnella casimirovensis Taxon-range-zone quence. At Beutenaken. the Beutenaken Member (not present in Halembaye and Beutenaken) lies on top of this hardground and contains Be Definition : Interval from the first to the last lemnella lanceolata inflata. When one takes into occurrence of Belemnella casimirovensis (SKOLOZ account the frequent occurrence and the condition of preservation of the guards. we are probably DROWNA, 1932). dealing with a condensed sequence. The Belemni Author: JELETZKY (1951 ). tes indicate that the Beutenaken Member has Lithostratigraphical correlation : Maastricht been deposited in the Lower Maastrichtian. Formation. uppermost part of the Meerssen The Beutenaken Member characterized by Be Member. lemnella lanceolata inflata is not present at Ha Age : Upper Maastrichtian (lower part). lembaye. On top of the Beutenaken Member is a bed with reworked guards of Belemnella "occiden talis". These guards are numerous in Beutenaken 5.1 .6. Conclusions and their presence is questionable at Halembaye. Perhaps we are dealing in Halembaye with guards The boundary between the Campanian and the of Belemnella cimbrica at the base of the Vijlen Maastrichtian is marked in Beutenaken as well as Member (SCHULZ & SCHMID. 1983). The Vijlen in Halembaye by a remarkable lithological discon Member is found on top of the Beutenaken tinuity consisting of a hardground (Froidmont Member at Beutenaken and on top of the Zeven hardground). With the discontinuity coincide : Wegen Member at Halembaye with occurrences - the extinction of both Campanian species of Belemnitella junior from the Upper Maastrich Belemnite//a mucronata and Be/emnitella mucro tian. nata "minor" at the top of the hardground capping the Zeven Wegen Member: - the appearance of the Lower Maastrichtian ACKNOWLEDGEMENTS Belemnella lanceolata inflata at the base of the Beutenaken Chalk at Beutenaken and the base of I wish to express my thanks to Dr. M.J.M. the Vijlen Chalk at Halembaye. Bless. Museum of Natural History at Maastricht; It is pointed out that only rare guards of Dr. J. de Vos. Teylers Foundation at Haarlem. representatives of the genus Belemnella were W.M. Felder at Vijlen for placing the studied found in Halembaye. So as Belemnella lanceolata material at my disposal. and Dr. W.K. Christensen inflata is very rare and reworked at Halembaye, for critical review of the text and specimens one may conclude that the Lower Maastrichtian is figured. BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 23

5.2. OTHER CEPHALOPODS 5.3. FORAMINIFERA (LA. VDT) AND OTHER MACROFOSSILS Foraminifera from the Late Cretaceous to Pa Apart from Belemnites, 12 species of Cephalo leocene calcilutites and calcarenites of Limburg pods occur in the localities Halembaye and Beute have been known for about half a century. Main naken. Only a small part of these species are studies were made by VAN R1JSINGE (1932. Foramini mentioned in (old) literature. In outcrops of the fera of the Houthem Formation), ScHIJFSMA (1946, Vaals Formation in the vicinity of Cottensen, . Foraminifera of the Vaals Formation), HoFKER (1949, Teuven and Vaals, the Lower Campanian Ammo 1955, 1956. 1957. 1958, 1961, 1966 :Foraminifera of noids Scaphites hippocrepis (DEKAY, 1827), Placen Late Cretaceous - Paleocene formations), MEIJER in ticeras meeki BbHM, 1898; Euhomaloceras incurva CALEMBERT et al., (1977, index benthic Foraminifera tus (DuJARDIN, 1837) and ? Sciponoceras bohemi from Late Cretaceous formations); BELLIER & VILLAIN cum (FRJTSCH, 1872), and the Lower Campanian (1975, planktonic Foraminifera); VILLAIN (1977, Nautiloid Epicymatoceras vaalsensis (B1NCKHORST, partly benthic Foraminifera); MEESSEN in STREEL et 1861) were found. In the Vaals Formation of the al., (1977, benthic Foraminifera, with use of the C.P.L. quarry at Halembaye the Nautiloids Epicy Bolivinoides lineage); MEESSEN et al., (1978); matoceras vaalsensis (B1NCKHORST, 1861) and Eu MEESSEN in BLESS et al., (1981); MEESSEN, ROBAS trephoceras depressus (B1NCKHORST, 1861) were ZYNSKI in ROBASZYNSKI et al.. (1985. preliminary found. In the Vijlen Member, the Maastrichtian results of the present work). Ammonoids Acanthoscaphites tridens (KNER, 1848) and Hoploscaphites constrictus tenuistriatus (KNER, 1848) were found in outcrops west of Beutenaken. 5.3.1. Benthic Foraminifera (J.P.M.Th.M.) In the Vijlen Member of Halembaye (Fig. 12), the The samples collected at Halembaye. Beutena Upper Maastrichtian Ammonoids Pachydiscus sp., ken and Cadier en Keer have been investigated on Hoploscaphites constrictus tenuistriatus (KNER, their benthonic foraminiferal content. The Forami 1848) and Hoploscaphites constrictus constrictus nifera were identified according to the criteria of (SOWERBY, 1818) NOWAK 1911, were found (VAN DER HoFKER (1957, 1966) and dated according to TuuK, in prep.). In the upper part of the Halembaye HoFKER's 1966 foraminiferal zonation. The Foramini quarry (Lanaye Member) several calcareous parts fera assemblages are listed in Fig. 16 and Fig. 17. of the cephalopod jaws Conchorhynchus limbur The dating of samples is also based on the gicus (vAN DER TuuK, 1982) and Rhyncolites mini orthogenesis of the Bolininoides decorata-austra mus B1NCKHORST (1861) were found. Among several lis-gigantea lineage (Fig. 15) as described in detail specimens of jawparts of Glyceridae (Polychaetia), by HoFKER (1958 a, 1961 ). The Foraminifera lineage there are a few specimens which might be hoo Bolivinoides decorata-australis-gigantea displays a klets of cephalopod tentacles in the Smectite gradually increasing number of pustules on the (Vaals Formation) of Halembaye. But this has not last chamber (HoFKER 1958 a. 1961). Bolivinoides been confirmed yet. It is pointed out here that all decorata possesses 3 to 4 pustules on the last the above mentioned Cephalopods are extremely chamber in Foraminifera Zone A. The mean num rare with the exception of the Ammonoids Scaphi ber of pustules on the last chamber of Bolivinoides tes hippocrepis and Euhomaloceras incurvatus australis increases from 4 to 5 in Foraminifera and that there are no other Cephalopods known in Zone B, through 5 to 6 in Foraminifera Zone C, and the Zeven Wegen Member, the Beutenaken 6 in Foraminifera Zone D, into 6 to 7 in Foramini Member and the Lixhe Member than Belemnites. fera Zone E. Eventually. Bolivinoides gigantea pos So one may conclude that Cephalopods other than sesses a mean number of 7 to 9 pustules on the Belemnites are not very useful for stratigraphical last chamber in Foraminifera Zone F. purposes in the Vaals and Gulpen Formations. According to literature, the vertical distributions Comments on the foraminiferal content of the of some Echinoids (after MEUER. 1965) and Bra samples studied chiopods (in ALBERS et al., 1978) are presented in Fig. 12. • Samples Halembaye 82-12 and 82-11 : Maastrichtian, Foraminifera Zone E. The following characteristic species have been recognized : Al lomorphina bullata. Neoflabellina reticulata. Prae bulimina laevis and Reusse//a cimbrica. In sample Halembaye 82-11. the mean number of pustules 24 F. AOBASZVNSKI ET COLL. BCREDP 9 (1985)

HOFKER' lithological s samples number of pustules on the last formed chamber averages units Zones 8

LIXHE E Halembaye 82-12 2 l------+-----1------Halembaye 82-11 24 14 6.2 D Halembaye 82-15 Halembaye 82-10 VIJLEN C Halembaye 82-9 20 17 5.5 Halembaye 82-8 3 ------+--Cadier------e.K. 75.9-77 m no Bolivinoides Beutenaken 82-1 Beutenaken 82-2 4.5 Beutenaken 82-3 no Bolivinoides BEUTENAKEN B Beutenaken 82-4 no Bolivinoides Beutenaken 82-5 no Bolivinoides Cadier e.K.78.95-80 m no Bolivinoides 1-----�------Cadier ------e.K. 80-81 m no Bolivinoides Halembaye 82-7 31 3.8 Halembaye 82-6 20 3.7 ZEVEN Halembaye 82-5 24 31 3.6 A Halembaye 82-4 18 13 3.4 WEGEN Halembaye 82-3 17 3 3.2 Beutenaken 82-6 no Bolivinoides �-----i------1------Beutenaken 82-7 ------Halembaye 82-2 no Bolivinoides VAALS Halembaye 82-1 no Bolivinoides number of specimens

FIGURE 15 The orthogenesis of the Bolivinoides decorata-austra/is lineage

on the last chamber of Bolivinoides australis is 6.2. chamber of 5.5. This value is within the range This value is within the range between 6 and 7 between 5 and 6 pustules. which HoFKER (1958 a. pustules. which HoFKER (1958 a. 1966) considered 1961) considered characteristic for Bolivinoides characteristic for Bolivinoides australis in Foramini australis in Foraminifera Zone C. Bolivinoides fera Zone E. Remarkable is the occurrence of draco has been recognized in this zone in at least Bolivinoides draco in sample Halembaye 82-11. one horizon. where the mean number of pustules • Sample Halembaye 82-15: Maastrichtian. on the last chamber of Bolivinoides australis is Foraminifera Zone D. The following "characteris about 5.4 (K1MPE et al., 1978). tic" species has been recognized : Bolivinoides • Samples Beutenaken 82-1. 82-2. 82-3. 82-4. draco. It should be noted - contrary to previous 82-5 and Cadier en Keer 78.95 m - 80.00 m and knowledge - that this species is not restricted to 80.00 m - 81.00 m : Maastrichtian. Foraminifera this Foraminifera Zone. but has also been recogni Zone B. The following characteristic species have zed in Zones C and E. been recognized : Eponides beisse/i, Neoflabellina • Samples Halembaye 82-10. 82-9 and Cadier praereticulata, Orbignyna aragonitica, Osangularia en Keer 75.90 m - 77.00m : Maastrichtian. Forami lens, Praebulimina laevis, Siphogaudryina (Hete nifera Zone C. The sample Cadier en Keer was very rostomella) foveolata, Spiroplectammina laevis poor and by that no characteristic species have and Verneuilina limbata. In sample Beutenaken been recognized. In the Halembaye samples the 82-2, Bolivinoides australis has a mean number of following characteristic species have been reco pustules on the last chamber of 4.5. This value is gnized : Bolivina incrassata, Neoflabellina praereti within the range between 4 and 5 pustules, which culata, Pseudoparrella alata and Bolivinoides aus HoFKER (1958 a. 1961) considered characteristic for tralis with a mean number of pustules on the last Bolivinoides australis in Foraminifera Zone B. BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 25

• Samples Halembaye 82-7, 82-6, 82-4, 82-3 ranging from the Campanian throughout the and Beutenaken 82-6 and 82-7 : Campanian, Fora Maastrichtian was found in the Zeven Wegen, minifera Zone A. The following characteristic Vijlen and Lixhe Members. G/obotruncana cf. ven species have been recognized : Gavelinella c/e tricosa and G/obotruncanita stuartiformis also mentiana, Gavelinopsis monterelensis, Globorota known in the Campanian-Maastrichtian are pre lites micheliniana, Neoflabellina leptodisca and sent in the Vijlen Member. A specimen close to Stensioeina pommerana. In the Halembaye sam G/obotruncanella petaloidea was picked out from ples, Bolivinoides decorata shows a mean number the Vijlen Member, and this species is restricted to of pustules on the last chamber from 3.2 to 3.8. the Maastrichtian, as Rosita contusa cited by These values are within the range between 3 and BELLIER & VILLAIN (1975) at the top of the Vijlen 4 pustules which HoFKER (1958 a, 1961) considered Member and at the top of the Lixhe Member. characteristic for Bo/ivinoides decorata in Forami It is obvious that the scarcity of planktonic nifera Zone A. Foraminifera in the calcilutites and calca·renites studied does not allow their use as biostratigra • Samples Halembaye 82-2 and 82-1 : Campa phical markers in the Limburg area. Only Globo nian, lower part of Vaals Formation. (the Foramini truncanella cf. peta/oidea and Rosita contusa sup fera of the Vaals Formation were described by port a Maastrichtian age for the Vijlen and Lixhe HoFKER in 1957). The following characteristic spe Members. cies have been recognized : Gavelinella clemen tiana and Lenticulina multinodosa. The foraminiferal zonation of HoFKER (1966) can be used successfully in the type-area of the 5.4. NANNOPLANKTON (H.M.) Maastrichtian and in adjacent parts of Belgium and the Federal Republic of Germany, but the Foraminifera Zones of HoFKER are Assemblage The Campanian-Maastrichtian boundary is so zones. Therefore, the vertical distribution of the mewhat difficult to recognize with nannoplankton "characteristic" species is not restricted to a single because of problems in determining the index zone, as can be deduced from the distribution species and possible diachronism of their appea charts (Fig. 16 and 17). Their vertical range has rances and extinctions from the Tethy�n to the been influenced to a considerable extent by Boreal realms. For example, PERCH-NIELSEN (1979, palaeoecological conditions. This reduces their 1983) considered that there are no good markers value for long-distance correlations (compare the to draw this boundary which falls into the Tranoli different opinions of HoFKER, 1966, and VILLAIN, thus phace/osus Zone. For THIERSTEIN (1978), the 1977, on the correlation between the Late Creta disappearance of Eiffe//ithus eximius would be a ceous of the Maastricht and Mons area). Important good datum-line, but the extinction of this form is for correlation, also with other basins (HOFKER, not synchronous everywhere. ROTH (1978) put the 1958 b; VAN H1NTE, 1967), is the Foraminifera li boundary in the Lithraphidites praequadratus neage Bolivinoides decorata-australis-gigantea. Zone. More recently, LAMBERT (1980) studied the nannoflora of the type-Campanian area and of some Limburg samples, and VERBEEK (1983) pre 5.3.2. Planktonic Foraminifera (F.R.) sented a zonation for the Campanian-Maastrich tian of South-Limburg. For the latter author, the The species of planktonic Foraminifera recove Beutenaken Member belongs to his Ouadrum red from the Halembaye and Beutenaken samples trifidum Zone which he assumed "to be of Cam are much less abundant than the benthic Foramini panian age". fera (Fig. 16 and 17). Very rare in the Zeven Wegen After examination of samples from Halembaye, and the Beutenaken Members, they are slightly Beutenaken and Cadier en Keer, the same species better represented in the Vijlen and Lixhe Mem described in previous works were recognized. It bers. seems that the datum-lines of several index spe Usually, Heterohelicids and Globigerinelloides cies are diachronous from the Tethyan to the have little biostratigraphical value. Only species of Boreal realms. Globotruncanids may provide some stratigraphical The nannoflora of the Cretaceous Limburg information in using their well-known ranges in the calcilutites and calcarenites is abundant rather Tethyan realm (ROBAS2YNSKI, CARON, GONZALEZ DO diversified, well preserved, with no evidence of NOSO, WONDERS et al., 1984). Globotruncana area reworking. Diagenesis is generally weak except for UPPER CAMPANIAN UPPER M A A S T R I C H T I A N ( pars) STAGES � ("") C HOFKER 's zones (1966) ZEVEN WEGEN Mpmber M.m�r I LI XHE 1 :I: Formal lithotype,s(FELDER,1975) > ,- M•tric seal• . :.•,. : ' .,', "1 LITHOLOGY I'•'I 3: ,. '. a, :I: �:I: � � � � :I: � J � � � N... � � SAMPLES I ...... � ao 2 ... I I I I I N•ofl•b•lliru sph.-noi,ulis (WEDEKIND) Globulin• li,crima REUSS G.nlin•U• inw,lul• HOFKER Cibicid•s ..cn•I• (BROTZEN) hnticulin• multinodou SCHIJFSMA

bnticulin• ordin•ris SCHIJFSMA G•v•lin•II• d•ini ( SCHIJFSMA) L.nliculin• (S•r•c•n•ri•) tri•ngul•ris (d'ORBIGNY) Frondicu l•ri• la•vig•I• MARIE ,, Globorol•lit.s mich.-lini•n• (d'ORBIGNV) 0 -- - - - m CD ITI - Gu•lin•II• cl•m•nfi•n• (d'ORBIGNV) - -1-- - CJ) - BROTZEN z N - St.-nsia.in• pomm•r•n• -4 -< (REUSS) Ammodiscus cr•l.c•us ::c CJ) - la•vis (BEISSEL ) � -I· Pr.. bulimiN 0 -1 - bnticulin• (S•r.c•n•ri•) trilob•I• (d'ORBIGNY) -I - () - - -- Gyroidinoid•s nit id• (REUSS) 0 -,-I - - - Cibicid.s subbosqu.ti HOFKER 23 I Cith•rin•II• gr•ciliN (MARIE) :::u Atuophr•gmium cr•ssum (d'ORBIGNY) )> � Bolivinoid.s l••vig•I• MARIE z _, Bolivinoid.s thcor•I• {JONES) -- - Angulog•v•liMlli, gr•cilis (MARSSON) L.nticulin• SK•ns (REUSS) :::u - - -1 I Orbignyn• v•ri•bilis (d • ORBIGNV) )> G•v•lin•II• lorMi•n• (d'ORBIGNY)

Gu•I inopsis voltzi•n• (d 'ORBIGNY) I -1 - - L.nticulina ps•udov•lis MARIE -I -- - Spiropl.cl•mmin• IHvis (ROEMER) _I CD -- - Oorothi• pupa ( REUSS) () I - :Il -I G•udryin• cr•l•cN (KARRER) "'O _1 - - Ga"lin•II• �rtCIU (MAASSON) I CD -i - -- 0.v.linopsia IHmbi• (MAASSON) -1 -- - 1"•r•son•II• oayco,.. (REUSS) : Tritaxia dubia (REUSS) CD () I N•oflab•llina l•plodisca (WEDEKIND) m:JJ t-��+-��+-��t·��- 0 1 Ga11•linopsis monl•r•l.nsis (MARIE) "'O -: Eponid.s b•iss.li SCHIJFSMA co - -I - Pull•nia am•ricana CUSHMAN Boli11ina d•curr•ns (EHRENBERG) : j 1 N•oflab•llina prur•liculata HILTERMANN CD I rn I Osangularia l.ns BROTZEN z I Orbignyna 011afa HAGENOW I � I L•nliculina (Astacolus) truncata (REUSS) ::c -1 Boli11inoid•s australis EDGELL n () - --1 - Boli11ina incrassata REUSS � � - -1 Ga11•linopsis complanata (REUSS) 'TI � - I - R•uss•II• er is ta ta (MARSSON) z 0 _I Siphogaudryina (H•t.rostom•II•) fo11.alata (MARS.) � I ::0 z (d'ORBIGNY - 1 Cibicid•s bNumontianus ) > � I Boli11inoid.s p•f•rssoni BROTZEN � Vl� I -l I - Alabamina dorsopl.-na (BROTZEN) z :JJ -I - Ps.udoparr•I� ala/a (MARSSON) 'TI nI - Frondicularia linguiformis MARSSON rn -l : ::0 - Gut tulina adha•r•ns (OLSZEWSKI ) z� I > Boli11inoid.s draco (MARSSON) CD t------�---1- • 1 - 0 I -- Dorothia pupoid.s (d'ORBIGNY) C • Abundant -1 - z - N•oflahllina r•ticulata (REUSS) 0 -common - I - � - Allomorphina bullata HOFKER :JJ -Pr•sent -1 -< I - Slilostom•II• spinosa (HOFKER) z -Rar• - R•uss.lla cimbrica (TROELSEN) m� J :JJ H•l•roh•lii striata (EHRENBERG) � complanata (MARIE) "lJ � Vl� Globig•rin.lloid.s gr. asp•ra (EHRENBERG) r- -l > :JJ cf. multispina (LALICKER ) I z n ::,; I Archa.oglobig,,t"ia cr•lacN (d'ORBIGNY) � -l d. blowi PE SSAGNO 0 Globotruncana cf. bulloid.a (VOGLER) z area (CUSHMAN) n lnt•nn. area- ros•lta rugosa (MARE) et. linn•ia,..-n-ntricou � Rosita contuu (CUSHMAN)ln BELLER& VILL 197S Globotruncanita stuartiformis ( DALBIEZ) � _l et. Globotruncan.tla P•laloi,,.. (GANDOLFI) l\l FIGURE 16 ...... Vertical distribution of benthic and planktonic Foraminifera for the Halembaye section � P- �d UPPER CAMPANIAN LOWER MAASTRICHTIAN STAGES UPPE CAMP. LOtl. T 11 �t � J> aJ N I 00 V. I ZEVEN WEGEN M. I BEUTENAK. M. fVIJLE N M. V. I ZEVEN WEGEN M•mt.r BEUTENAKEN M•mb« HOFKER 's zones I FormAI lithotypes (FELDER,1915) 11 '. -� �tric seal• .. ' . · 1 • '' l.l ...3 .. ', ·, ..'. ' ';:.,\ [... ,/ LITHOLOGY ,' ID ID ; Ill I'll Ill C "' C ..... � O�Oal C C 3 �O;;f � � ,... :-4 g · g � � SAMPLES ·g � ... : ...; � Al••ophr•gmium globosum (HAGENOW) VPrn.uilin• limbal• Orbignyn• •r.gonitic•CUSHMAN HOFKER Bolivin• pl•it• Frondicul•ri• ogiv•lisCARSEY MARIE Allomorphin• •llomorphinoid•s SIPnsio•in• pomm•r•n• (REUSS) G•v•lin•II• lornPiu1• BROTZEN N•ofl•Mllin• prHrPlicul•I•(d'ORBIGNY) G•v•linops is voltzi•n• HIL TERMAN - (d • ORBIGNY) OJ Eponid•s b•isuli SCHIJFSMA 11'1 ,, 0 CD Os.ngul•ri• l•ns z :::0 )> n, Orbignyn• oval• BROTZEN 0 C, HAGENOW ---t OJ C P,.,.bulimina ,.,.vis ( :c }> BEi SSEL) en ---t L•nticulina (S•r•c•nari•J trilob•I• n. n, (d'ORBIGNY) n, GyroidinoidPS nitid• z ::0 - z (REUSS) en - Cibicid•s subbosqu•li � HOFKER )> L•nticulin• ps•udov•lis m n, MARIE -I z ::,;; Spiropl•cl•mmina ,.,.vis Dorothi• puf'_• (ROEMER) () n, 0 z (REUSS) ::0 r G•udryin• cr•l•c,.. )> ! A G•v•lin•II• p•rlus. (KARRER) n, 0.vPlinopsis bPmbi11(MARSSON) z n, M•rsson•II• 011ycon•(MARSSON) ::0 Pull•ni• •m•ric•na (REUSS) CUSHMAN � BolivinoidPs •uslr•lis Bolivin• incr.ss.t• EDGELL ::0 G•11•linopsis compl•REUSSn•I• )> (REUSS) R•uss•II• crisl• I• ( Siphogaudryina(H•l•rostom•ll•J MARSSON )fov•ol•I• (MARS.) Orbignyna v•ri•bilis ( • Abundant G•11•li11PII• clPmPnti•n•d'ORBIGNY) (d "OR BIG NV) - Common Globorot•lil•s mich•lini•na - Prt'sent Ammodiscus cr•f•c•us (d'ORBIGNY) - Rarl' G•11•linopsis mont•r•l•nsis(REUSS) OJ () (MARIE) :::0 N.afl•b•llin• l•plodisc• m Trit.. i• dubi• (WEDEKIND) 0 ( -0 Bolivinoid•s d•cor•REUSS) I• (JONES) co Arch.,.oglobig•rin• blowi :tJ PESSAGNO :11 FIGURE 17 J Vertical distribution of Foraminifera for the Beutenaken and Cadier en Keer borehole sections STAOl!S UPPER CAMPANIAN M A A S T R IC H T I A N (pars) CJJ 0 'TI HOFKER 's zonH ( 1966) n:c ZEVEN WEGEN M.mt>.r M.mi>•r I LI XHE 1 LAHAYE M.nt,. Formal llthotype(FELDER,1975) m ::c 0 > M•trlc seal• "'tl r . :.• .. : . m LITHOLOGY co I::'.! :I: a, � J ri � � � � 1 NN N e IS e N! � �:: e r: SAMPLES I!' ..�,,I I .• :: ,; I!' .:. .i NW .. .;, "' ..:. IO � 13 13 IIL.!.., � I I I ..... !... .!_ I !..._. f> '(' Rrinh•rdtitrs •nthophorus DEFLANORE I I Tr•nolithus orioNtus STOVER I Amphizygus minimus BUKRY Broinsoni• /»fa constrict• HATTNER f'l al. Eiffrlithus rrimius (STOVER) n - _J )> - Luci•norh•bdus c•yruri DEFLANDRE � - Ph•nulitrs obscurus (OEFLANDRE) - - - - � (DEFLANDRE) � - - Qu•drum gothicum 1 - z -, - G•rtn•r•go obfiquum (STRADNER) )> - ->Ahmurlrrrl • octor•di•t•(GORKA) t------+------;e------...,______- l z ---1 - -> Biscutum const•ns (GORKA) z � � -' - - ->Broinsoni• rnormis (SHUMENKO) _J - -> BRAM. & MART. )> UJ� Chi•stozygus •mphipons -I - - ->Crrt•rh•bdus conicus BRAM. & MARTINI � - - :c 1 ->Crrt•rh•bdus crrnul•tus BRAM.& MARTINI z nI _J - - ->Cribrosph••r•fl• frltrnbrrgi (ARKHANGELSKY) -I 1 - ->Discorh•bdus ignotus (GORKA) z )> - - ->K•mptn•rius magnificus DEFLANDRE 0 z � CJJ -, - - -> Eiff•lfithus turrisriffrli (DEFL.& FEAT) DEFLANDRE 0 ->Lithrap_hiditf'S carniolrnsis "1J C _J ->ManiYitrlfa prmmatoidH (DEFLANDRE) z _J r- 0 ->Markafius circumradiatus (STOVER) )> ...J ->Microrhabd ufus drcoratus DEFLANDRE :c - )> -< - - (GARDE T) ------>Micula staurophora z - ARKHANGELSKY) - -- - -> Prrdiscospharra crrtacu ( z m )> I ->Prrdiscospha•r• Spinosa BRAM. & MART. :c � ->Vrkshinrlla stradn•ri ROOD •t al. � ->Watznau•ria barnrsa• BLACK � • - _J --t - 1- - - REINHARDT ->Watznaurria d1111rbulf.ryi -I UJ� >Zygodiscus spiralis BRAM. & MARTINI 0 -I I Arkhangrlski•ll• sprcillata VEKSHINA :c ---1 - >Microrhabdulus stradnrri BRAM. & MARTINI z nI --i Acuturris scotus RISATTI -I � ->Eiffrllithus gorkar (REINHARDT) I ->Cylindralithus s•rratus BRAM. & MARTINI -, Prrdiscospharra stovrri ( PERCH - NIEL.) -, ->Arkhangrlski•lla cymbiformis VEKSHINA - (STRADNER) • Abundant I Crratolithoid,s acuf•us --i Lithraphiditu pra,quadratus ROTH - Common � Rtinhardtitts lt11is PRINS & SISSINGH - Pres•nl I Quadrum trifidum STRADNER - Rar• _J et. BRAM . MART. I - > Thoracosphura op ,rculata & - >Lithraphiditu quadratus BRAM. & MART. Pr«llscosp. Broinsonia parca const ricta Zone stoveri z. 1 Lithraphidites praequadratus Zone Lithr. quadratus Zone ZONES I\J FIGURE 18 CJJ HOF KER 's zones 0 V. I ZEVEN WEGEN M. I BEUTENAK. M. I VIJLEN M. V. ZEVEN WEGEN M•mti.r BEUTENAKE N M•mb•r _...__ Formal lithotypes (FELOER,1975) hr+-...... __,...__,___._.._...... _..,..,__...._ __._...... _..__, _...... , _.,_ ....,_...__ , ...,.... , Metric scale • · ' • I " \• · • • •-�� ..• ' , . · 1 • 1:V· :I-�-·�::::,,·:.:__ -�-�-�--_,,./ LITHOLOGY 1 �,, ffl ffl ffl ffl ffl fflIll � a goat jO� ·s g ! � � � � � � � SAMPLES ·g 1R :et I � �f :sI I �I � ..... 0, UI ._ W N - < - -- _l R•inhardtit.s anthophorus DEFLANDRE < - -- l rranolithus orionatus STOVER < - - Amphizygus minimus BUKRY < - - -- Broinsonia pared constrict• HATTNER f't .al. < - --- Eiffrllithus •x imius (STOVER) < - - - - - L U --,.- -,.- -x_ _DE______- - ucianorhabd s , uDEi FLANDRE < ------Phanulit•s obscurus ( FLANDRE) < - - - Qua drum gothicum ( DEFLANDRE) < ------> Garfn•rago obliquum (STRADNER) < ------>Ahmurl•r•li• ocf oradiata (G ORKA) < ------> Biscutum constans (GORKA) Z < ------>Broinsoni• •normis (SHUMENKO) < ------>Chiastozygus amphipons BRAM.& MART. )> ("') < CD ------>Cr•tarhabdus conicus BRAM. & MARTINI z :n < - ---- >Cr•f•rhabdus cr•nulatus BRAM.& MARTINI :0 )> r11 0 CJ < C ------>Cribrospha•r•II• Prl'l•nb•rgi (ARKHANGELSKY) z CD :t> rn < -t - -- - >Discorhabdus ignotus (GORKA) CJ) < n, ------>Kampfn•rius magnificus DEFLANDRE Q• :::0 < -- • - - - - - • >Eiff•l{ithus turris•iff•li(DEFL.& FERT) z < Z - - - - - • >Lithraphiditu carnio/Msis DEFLANDRE '1J CJ)� rn < )> ------>Manirit•II• p•mmafoid•a (DEFLANDRE) m < 1 -I :,:; ------> Marlcalius circumradiatus (STOVER) () < n, - >Microrhabd ulus dMoratus DEFLANDRE 0 < ------• >Micufa staurophora (GAR DET) )> r z ------! :,; < -· • >Prrdiscospha•ra cr•tacu (ARKHANGELSKY) z rn < - - -- >Pr•discospha,ra Spinosa BRAM.& MART. rn < - ---- >V•kshin,({a stradn,ri ROOD et al. :,:; :::0 < - - - -- • -- >Watznau,ria barn,sa, BLACK < -· - ---- Wafznau,ria dar•bukryi REINHARDT -t - - > ---- >Zygodiscus spirafis BRAM. & MARTINI Q < - - Arkhang,tskirlla sprcilfata VEKSHINA < ------>Microrhabdufus stradn•ri BRAM. & MARTINI Z < - - --- Acuturris scotus RI SATTI ------>Eiff•lfithus gorkar (REINHARDT) < - - - - Cylindralithus srrrafus BRAM. & MARTINI < - ---- Prrdiscospharra stor•ri ( PERCH-NIEL.) • Abundant - - • ------>Arkhangrlskirlfa cymbiformis VEKSHINA - - C•ratolithoid.s aculrus ( STRADNER) -common ----- Lithraphidites praequadrafus ROTH -Present - - --- >Reinhardtites l•ris PRINS & SISSINGH CD -Rare - Quadrum trifidum STRADNER () :Il - - - > Thoracosphaera et. operculata BRAM. & MART. m >Lithraphidites quadratus BRAM. & MART. 0 ! "'O llith. praequadratus Broins. parca Pred. stoveri I Lithraphidites praequadrat\.111 : ZONES co Zone const. Zone : Zone Zone 1 FIGURE 19 I Vertical distribution of calcareous Nannoplankton in the Beutenaken and Cadier en Keer sections BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 31 some local secondary calcite recrystallizations Prediscosphaera stoveri and Ouadrum gothicum. (Fig. 18 and 19). The species Lithraphidites praequadratus beco mes more frequent and at the top appears Lithra 5.4.1. Main biostratigraphical results phidites quadratus.

The Vaals Formation contains a nannoflora 5.4.2. Biozonation principally composed of Broinsonia parca constricta, Broinsonia enormis, Lucianorhabdus • The [Jroinsonia parca constricta Zone (author cayeuxi linked with Phanulites obscurus, Watz of the B. parca Zone : S1ss1NGH, 1977; emend. CRUX, naueria davebukry,� Watznaueria barnesae, Micula 1982). It is the interval between the appearance of staurophora, Reinhardtites anthophorus and the index species and that of Prediscosphaera abundant Eiffellithus eximius. stoveri. This definition follows that given by CRUX The assemblage belongs to the Broisonia parca (1982) which I use in the Paris Basin (and not that constricta Zone which, in Charentes. is C.ower to proposed by THIERSTEIN, 1976 and VERBEEK, 1977). At Middle Campanian. Halembaye. Prediscosphaera stoveri appears in The Zeven Wegen Member at Halembaye and the last third of the Zeven Wegen Member. Beutenaken is marked by some changes : • The Prediscophaera stoveri Zone (author: - Eiffellithus eximius becomes much less abun LAMBERT, 1980). In Limburg it is the interval bet dant; ween the appearance of the index species and that - Cylindralithus serratus and Eiffellithus gorkae of Lithraphidites praequadratus. In the Tethyan appear at the base of the Member; realm, VERBEEK (1977 and 1983) proposed a Qua drum gothicum Zone (interval between the appea - at the top of the Member the entry is noted of rances of Ouadrum gothicum and Ouadrum trifi the first and still rare Arkhangelskiella cymbiformis dum) in place of the P. stoveri Zone. This zone is and Ouadrum gothicum; not used in Limburg because of the scarcity in the - Prediscosphaera stoveri appears in the upper Boreal realm of both 0. gothicum and 0. trifidum. part of the Member (in the Charentes, this species Although the extinction of 0. trifidum has been appears in the Middle to Upper Campanian). used in the Tethyan realm to place the Campa The Beutenaken Member was studied on sam nian-Maastrichtian boundary, this species is so ples coming from Beutenaken and from the Cadier rare in the Boreal realm that it has little value. But en Keer borehole. The species Broinsonia parca it is worthy of note that this species is present both constricta and Eiffellithus eximius whose extinction in the Beutenaken Member and the Vijlen Mem is generally considered in the literature as marking ber. The distribution of P. stoven: a small form not the Campanian-Maastrichtian boundary are pre always differentiated from P. cretacea, does not sent in the Beutenaken Member. as well as Qua seem latitudinally controlled. This species has been drum trifidum. The two species Lucianorhabdus found in England (CRUX, 1982), in Charentes (LAM cayeuxi and Phanulites obscurus are also present BERT. 1980) and in the Paris Basin (personal data). but less frequent. The species Lithraphidites prae • The Lithraphidites praequadratus Zone (au quadratus and Reinhardtites levis appear at the thor : ROTH, 1978). It is the interval between the base of the Member. appearance of the index species and that of Li At the base of the Vijlen Member, several thraphidites quadratus. Lithraphidites praequadra species such as Broinsonia parca constricta, tus is a small form evolved from Lithraphidites Eiffellithus eximius and Reinhardtites anthophorus carniolensis and it is not largely used because it disappear. In the Tethyan realm the extinction of seems to be absent in the Tethyan realm although these species is considered as marking the Cam LAMBERT (1980) found it in Charentes. The zone can panian-Maastrichtian boundary. Two possibilities be considered as an equivalent of the Arkhange/s can be evoked to explain their presence in the kiella cymbiformis Zone sensu PERCH-NIELSEN Vijlen Member (which is Upper Maastrichtian by (1972) or sensu MARTINI (1976), but not sensu the occurrence of numerous Be/emnitella junior ) : SISSINGH (1977). either these species are diachronous from the • The Lithraphidites quadratus Zone (author: Tethyan to the Boreal realms, or they are reworked CEPEK & HAY. 1969; emend. PERCH-NIELSEN, 1977). It (but there is no evidence of reworking). is the interval between the appearance of the At the base of the Lixhe Member. Lucianorhab index species and the appearance of either Micula dus cayeuxi and Phanulites obscurus disappear, murus in the Tethyan realm or Nephrolithus fre and below the top of the Member disappear q�ens in the Boreal realm. The index species 32 F. ROBASZYNSKI ET COLL. BCREDP 9 (1985)

L. quadratus was found at Halembaye near the to" this formation (especially Palaeohystrichophora of the Lixhe Member. infusorioides, Spinidinium angustispinum in WIL SON), about ten of them disappear at the base of the Zeven Wegen Member (Acanthaulax saetosa and Gonyaulacysta prominoseptata inWILSON, Tha 5.5. DINOFLAGELLATES (J.-C.F.) lassiphora? spinosa. etc.). - Zeven Wegen Member {Upper Campanian). 5.5.1 . Previous work The species Dinogymnium euclaense, Exocho The first studies to obtain an accurate stratigra sphaeridium ? acuminatum in WILSON, F/orentinia ? phical distribution for the dinocysts fossilized in flosculusand Phanerodinium fourmarieri have only the Campanian-Maastrichtian chalky facies in been found at the base (sample HAL. 82-3). and Belgian and Netherlands Limburg were led by Laticavodinium gracilispinosum in WILSON only in W1LSON (1971, 1974). Previously, the observation of the upper part (samples HAL. 82-5 and 6). Many flints collected in several points of this region specimens of Gillinia hymenophora are present at (particularly in Loen, Halembaye, Gulpen) had the base and also in the upper part. On the other allowed LEJEUNE-CARPENTIER (1937-1951), CONRAD hand, Odontochitina wetzeli in WILSON has been (1941) and DEWIT (1943. 1944) to describe more or seen in all of the six samples. less accurately a small number of dinocyst forms. some of which being characteristic of these levels. - V,j/en and Lixhe Members {Upper Maastrich tian) More recently, SCHUMACKER-lAMBRY (1977) briefly reported the results of her own observations and Northidinium perforatum in WILSON and Klei compared them to W1LsoN's data. But the diffe thriasphaeridium cf. truncatum are present both in rence in the sampling has resulted in limiting the the Vijlen Member and the Lixhe Members. The comparison. Moreover, in both cases, the small Vijlen Member has given some specimens of number of samples produced a lack of precision Triblastula utinensis (samples HAL. 82-9 and 10) about the distribution of the diverse forms which and rather numerous specimens of Areoligera were found. tenuicapillata. Finally, the exhaustive study of the dinocyst The Cadier en Keer borehole (Fig. 21 ). content of some flints taken in comparable forma tions of the Mons basin can be noted (FoucHER & - Beutenaken Member {Lower Maastrichtian) ROBASZYNSKI, 1977). 33 genera and 45 species or subspecies of dinoflagellate cysts have been numbered in the 5.5.2. Analytical results of the present study two samples of the Beutenaken Member. We can note the presence in this chalk of The Halembaye quarry (Fig. 20). Cannosphaeropsis utinensis. Gillinia hymeno The Campanian-Maastrichtian sediments of the phora, Hystrichodinium pulchrum, Odontochitina Halembaye quarry are generally very fossiliferous : operculata, Palaeoperidinium pyrophorum, Xenas up until now 52 genera and 83 species or subspe cus ceratioides, Cyclonephelium distinctum, Sam cies of dinocysts have been recognized. 60 spe landia solida in WILSON and Spongodinium deli cies or subspecies, belonging to 37 genera. have tiense. been counted in the two samples of "Smectite" (Vaals Formation). 54 (33 genera) in the six sam - Vijlen Member {Upper Maastrichtian). ples of the Zeven Wegen Member, 35 (23 genera) Only one sample was studied and its dinocy�t in the three samples of the Vijlen Member, 23 population is qualitatively poor : 13 genera and 14 (14 genera) in the two samples of the Lixhe species or subspecies. Member. The following forms: Cyclonephelium distinc Characteristic forms for the different terms of the tum, cf. Spongodinium delitiense, Heterosphaeri section. dium ? heteracanthum and Pterodinium cingula tum cingulatum have not been identified in the - Vaals Formation : "Smectite" {Lower Campa equivalent strata of Halembaye. nian). Amongst the numerous species which have been identified. one third is exclusively present in BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 33

sary to notice in the Beutenaken Member the The Beutenaken quarry (Fig. 21) appearance of the following species : Palaeoperi The seven samples from the abandoned quarry dinium pyrophorum, Samlandia solida and Spon of Beutenaken have only given a limited and badly godinium delitiense, which confirms W1LsoN's data preserved population of dinocysts. no doubt due for this area. to weathering. 5.5.4. Remarks - Zeven Wegen Member (Upper Campanian) 16 genera and 18 species are represented in The stratigraphical distribution of several spe the two samples which have been analysed. all of cies may not be accurate. reworking being always them being present in Halembaye. possible. The reappearance after a variable length of time of a species represented by rare and badly - Beutenaken Member (Lower Maastrichtian) preserved specimens can be a sign of reworking. The examination of five samples has allowed It might be so for Odontochitina costata, Xenascus one to count 18 genera and 22 species or subspe ceratioides, Heterosphaeridium ? heteracanthum, cies of dinocysts. and to add some species to the Florentinia ? truncigera, Cal/aiosphaeridium inventory previously mentioned. In the Cadier en asymmetricum. Xiphophoridium alatum. Florenti Keer borehole. the noticeably missing species nia buspina, 0/igosphaeridium prolixispinosum, etc. were : Heterosphaeridium ? heteracanthum, Chy troeisphaeridia solida in WILSON. Odontochitina The stratigraphical distribution of the 14 chosen wetzeli in WILSON. Senoniasphaera reticulata in dinocyst species (Fig. 35) is not exactly the same WILSON. Cleistosphaeridium ? multifurcatum, Chy according to authors and countries. However, the troeisphaeridia everricu/a in WILSON. comparison of the various data allows one to select some species in order to situate an ap proximate Campanian-Maastrichtian boundary for 5.5.3. Biostratigraphical dinocyst species Western Europe. Thalassiphora ? spinosa disap pears during the Upper Campanian; so does Pa Thus. in the present case. we can draw three laeohystrichophora infusoriodes generally. whe zonal limits with the dinocysts. reas Spongodinium delitiense appears in the • The first limit corresponds to the Vaals uppermost Campanian or in the basal Maastrich Formation-Zeven Wegen Member boundary (or tian. Triblastula utinensis. on the other hand. is a Lower Campanian-Upper Campanian boundary) typical Maastrichtian species. and is marked by : the appearance of Odontochi tina wetzek Gillinia hymenophora and Chytroei sphaeridia solida; the disappearance of Palaeohys 5.6. trichophora infusorioides and Spinidinium angus SPORES AND POLLEN GRAINS (O.L.) tispinum. 5.6.1. (Fig. 22); • The second limit is situated in the upper part Halembaye quarry of the Zeven Wegen Member (below the Campa Although the samples from the Gulpen Forma nian-Maastrichtian boundary) and is characterized tion in the Halembaye quarry (HAL. 82-3 to by: the appearance of the genera Areoligera (es HAL. 82-12) contain a large number of dinoflagel pecially with the species senonensis and coronata) late cysts. they are completely barren in Spores and Cladopyxidium. the disappearance of Aldorfia and pollen grains. apart from a few very rare deflandrei. elements of terrestrial origin which have been • The third limit corresponds to the Beutena reworked from older horizons. Only the two sam ken Member-Vijlen Member boundary (Lower ples from the Vaals Formation. at the base of the Maastrichtian-Upper Maastrichtian boundary) and section. have yielded material of terrestrial origin. is shown by: the appearance of Northidinium although relatively little compared to the material perforatum; the disappearance of Odontochitina of marine origin. This material represents about operculata, Hystrichodinium pulchrum, Gillinia 20 % in HAL. 82-1 and 30 % in HAL. 82-2 of the hymenophora, Odontochitina wetze/i, and proba palynological content. Dinoflagellates accounting bly Xenascus ceratioides. for almost all the remainder. The Campanian-Maastrichtian boundary. such These Spores and pollen grains have been the as it is defined in the third chapter. is not clearly subject of preliminary inventories by VANGUESTAINE indicated by the dinocysts. However. it is neces- t1966) and VANGUESTAINE & STREEL ( in STREEL et al., UPPER CAMPANIAN �-Ml UPPER MAASTRICHTIA N (pars) STAGES m HOFMER 's zorws1966) ( w ZEVEN WEGEN M.m�r I VIJLEN M•mb•�ILIXHE 1 I LIXHE 2 l LIXHE 3 I L»4A� M.ri>. Forni.A llhotype(FELDER,1975) � :z: M•trlc se&I• I "' LITHOLOGY

>:J: I i i ii � �� r r r � r � � � "' SAMPLES ,IS N N IS :: I ...... o o . � .. .. � � �-. .:. ::S a, co = ...... ;, 0 13 :.I .. I I I I I I I I I I I < ------> Cl•istosph••ridium .,,,,.rum and d. (DEFLANDRE) < - d- - Coronif•r• ocHnic• COOKSON & EISENACK < • • -• - - - - Coronif•r• striol•I• (OEFLANDRE) - • • • • • (CLARt Hystrichosph.. ridium s.lpinr,ophorum DEFLAt«>RE < - • - - • • • • > Hyslrichosph.. ridium tubif•rum (EHRENBERG) < • - - • • - • • • • • > Hystrichosph••ridium ? p•lm•tum (WHITE ,1842,H BRON.) < - - -- - • • - • Kl•ifhri•sp,,.•ridium loffr.nH DAVEY & VERDIER < (WHITE) - • • • - • • - • • > Oligosph.. ridium compl.x 0 < - - - Surculosph.. ridium? longifurutum (FIATION) • - - -- - TI < • - - r.nyosp,,..,idium •ri•ulamum and d. DAV.& WILL.In D. •t al. - - - - • - :::0 < - - - C•ssiculosph.. ridi• et. r•ficul•f• DAVEY 0 - - z CD <; • • • - Odontochitin• cosf•t• ALBERT'l,1961,ern.nd. CLARt 0 (/) <; • • - - • - > Achomosph••r• r•mulif•r• (DEFLANDRE) < • - - • - - > Spinif•ritu r•mosus runosus (EHRENBERG) 'TI - (/) < - > Spinif•rifH r•mosus gr•cilis (DAV. e,t WILL. in DAV. et al.) • - • • - d- - • • - - > "Gony•ul•cyst•" w•fnlii ( LEJEUNE - CARPENTIER) • < m • • • • • - - X•Nscus c•r• fioid•s ( DEFLANDRE) > -l < () - • • - • • > Cyclon•ph•lium distinctum DEFLANDRE & COOKSON 0 < (DEFLAt«>RE C) r - • • • - - H•f•rosph••ridium?h•f•r•c•nlhum & G> r < • - • • • Hystrichodinium pulchrum DEFLANDRE Odontochitin• op•rcul•I• (0. WETZEL) fTI - cf - cf-• • • - < - • • A ldorfi• d•fl•ndr•i (CLARKE & VERDIER) r- < - - Flor•nfinia? truncig•r• ( DEFLANDRE) - • - • SMoni•sph.. r• profrUSll In WILSON r- < - - C•l•iosph.. ridium?•syrnm,lricum(DEFLANDRE & COURTEV.) > < - - > E11ochosp,,.•ridium? ps.udhystrichodinium (DEFLANDRE) < - - R•phidodinium fuc•fum DEFLANDRE -4 < Trichodinium c.sf•n•um DEFLANDRE - cf- - fTI < - Dinogymnium d•nficut.tum (ALBERTI) Ac•nfNulu s.•fos• in WILSON • -- Ch•f•ngi•I• spp . Dinogymnium spp. CD Gony•ul•cyst• prominos•pf•f• in WILSON () :::0 < • > Spinif•ritrs psf'Udofurc•fus ( KLUMPP) m < • > Spinif•rif•s r•mosus gr•nosus(DAV.& WILL. in DAY. •t al.) 0 < - Th•lassiphora ?spinosa (CLARKE & VERDIER) '""O (0 < Cf. Dinopf•rygium cl•doid•s DEFLANDRE ------··- -- > < • • I > Flor•nfini• f•ro11 ( DEFLANDRE) < - - I > Hystrichosph.. ropsis ovum DEFLANDRE I < • Js.b•lidinium cooksoni•• (ALBERTI) < - Cf. I (OEFLANDAE) < - - 'Microdinium"v•llg•rum DEFLANDRE PM#l!IOhystrichophora infusorioid.s < >I (0. WETZEL) Pterodinium cingufAtum cingulatum CD • in WILSON () < Spinidinium angustispinum :JJ - >I (DAV.& WILL. in DAV. et al.) m < Spinif•ritesCf. ramosusalatum(COOKSON mulfibrevis & EISENACK) 0 "'O < - Xiphophoridium (DEFLANDRE & COOKSON) _L >IAchomosph.. ra crassipellis CD < sagena DAVEY & WILLIAMS in DAVEY et al. >IAchomosphaera EVITT,CLARKE & VERDIER < Dinogymhiumtenera acuminatum (DAVEY & VERDIER) j < Florentinia DEFLANDRE < • PhanerodiniumSenoniasphaera setifer um CLARKE & VERDIER rotundata < - I (DAV.& WILL. in DAV. et al.) < > Spiniferites ramosus reticulatus (DEFLANDRE & COOKSON) - - - et- I I < - - > Oligosphaeridium pulcherrimum AGELOPOULOS < I Hystrichostrogylon membraniphorum • - Senoniasphaera in WILSON () reticulatasp. l> l Palaeoperidinium � < r: CLARKE & VERDIER Chlamydophorella discreta in WILSON z < Microdinium et. obscuriplicatum(ROSSIGNOL) )> < >>I Spiniferites membranaceus(C LARKE & VERDIER) � � - - • Spiniferites scabrosussp. et. in WILSON � < Adnatosphaeridium A. aemulum � - >I (D.& W. in D. et al.) CJ') ef-- Hystrichosphaeridium tubiferum brevispinum -i t. - • in WILSON :JJ �- . • • Chytroeisphaeridia solidain WILSON n Odontochitina wetzeli I • COOKSON & EISENACK -i • • Gillinia hymenophora in WILSON � et_ Senoniasphaera alveolata z < COOKSON EISENACK CD Dinogymnium euclaense in& WILSON 0 < Exochosphaeridium? acuminatum(DEFLANDRE ) C z < Florentinia ? ffoscufus LEJEUNE -CARPENTIER 0 Phanerodinium fourmarieri l> E • • I in WILSON • :JJ < - Chytroeisphaeridia everricula -< - >I (DEFLANDRE) < - - z Cleistosphaeridium?ef. multifurcatumCOOKSON & EISENACK m Canningia co Uiveri in WILSON l> - :JJ • Laticavodinium gracifi(0.spinosum WE TZEL) ·1· • • • • >I> Areoligera corona ta • • • LEJEUNE -CARPENTIER • • • • Areolig_era senonensis I spp. CJ')� - • • -i ·1· • • Cladopyxidium •• • • I - • sp . :JJ Xenikoon spp. n - - I I . - - • Areoligera in WILSON -i - - l - Northidinium perforatumef. ( BENSON) Kleithrias�haf'ridium truncatum - . ( 0. WETZEL) Arf'oligera tMuicapilfata0. WETZEL Triblastula utinensis DAV. & WILL. in DAV. et al. < >>I Cordosphaeridium fibrospi(CnosumOOKSON & EISENACK) < Leberidocysta chfamydata(DEFLANDR E) Phanf'rodinium cayeu,cii L_ L_ • Abundant • Common • Present - Rare Ch�isphaeridi'a solida genus Areoligera OiJontochitina Wf'lnli genus Cladopyxidiumsp. LAppearances __JExtinetions Gillinia hymf'nophora Xf'nilcoon __J L < Present in ante-Campanian of western Europe ,re}an . Northidinium perforatum w Palffohystrichophora infusorioicJ«.tdor f. ,a d• r•, >Present in post-Maastrichtian of western Europe U1 Spinidinium anguslispinum

FIGURE 20 Vertical distribution of dinoflagellate cysts in the Halembaye section P MA T STAGES E CAMP. . S �q UPPER CAMPANIAN LOWER MAASTRICHTIAN 11 UR> � ILOW.:"5 t � I J> m w HOFKER's zonPs V. I ZEVEN WEGEN M. I BEUTENAK. M.--iVIJLEN M. v. I ZEVEN WEGEN M•m�r BEUTENAKEN M•mb•r a> I I I Formal lithotypes (FELDER, 1975) Metric seal• ,,' :-.',' ... . . -�. ·.:.' .. ,·1 · ,.,, ··'_.' 1 ,/ LITHOLOGY 11 ·· -� . � ' .. . ' m ID m m m Ill m 111 m "' m RI !?O�Oal C: C: C: C: :jO� �r :-4 :-4 ,... s ,... s g 8 � ·g g � � ij SAMPLES � OI � ;.. z N � • - cf_ Achomospha,ra ramutifua (DEFLANDRE) Achomospha,ra sag,na & - DAVEY WILL. in DAVEY Pt al. Adnatospha,.ridium cf. A. a• mulum - A,,.otig ,.,a corona tasp. (0. in WILSON . - - • • WETZEL) - - Ar,olig,ra s•non,nsis -- . - LEJEUNE -CARPENTIER - - - Ar,.otig•ra f,nuicapiUata (0. Cannospha•ropsis utin,.nsisWETZEL) 0. ChatangiP/fa sp . WETZEL Pm. DUXBURY • • Cladopyxidium -- . • • spp . - - CfPistospha,.,idium armatum and cf.(DEFLANDRE) Coronif•ra striolata CD - (DEFLANDRE) () D•ffandrf'a spp. )> rn ExochosphHridium bifidum & CJ . - cf- - (CLARKE VERDIER) :0 - - - ExochosphHridium phragmif,-s al. DAV .al .t 0 · C� • DAVEY Pt in CD rn Exochosphaf'ridium? ps•udhystrichodinium :t> - (DEFLANDRE U) ::0 rn Ffor•nfinia buspina & N (DAVEY VERDIER) -< z From..a . z GiUin1'"a hymsp. Pnophora & U) rn . - )> COOKSON EISENACK � z Hystrichodinium pulchrum m rn Hystrichospha•ridium salpingophDEFLANDREorum -i - DEFLANDRE () •• z - Hystrichospha,.ridium tubif•rum 0 :,; (EHRENBERG) r rn - Hystr. tubif ,.rum br,.rispinum r /sab,.lidinium cooksoniaf' (D. & W. in D. et al.) rn •• (ALBERTI) ::0 L•b•ridocysta chlamydata & (COOKSON ElSENACK) Microdinium cf. obscuripficatum ------in WILSON Microdinium - spp. • Odontochitina op ,.rculata ( 0. . - • • • WETZEL) - •- - •- - Otigospha,.ridium compf•x - (WHITE) Oligosph. profixispinosum & DAV. WILL. in DAV. et al. • Pala..aperidini1111 pyrophor um ( EHR EN BERG) Spiniff'rif•s m•mbranac•us - (ROSSIGNOL) • • • Spinif•rit•s ramosus gracilis Sp. ramosus granosus ( (DAV. & WILL. in DAV. e-t al.) DAV.& WILL. in DAV. e-t al.) Sp. ramosus multibr•ris ( Sp. ramosus ramosus DAV. & WILL. in DAV. et al.) - - (EHRENBERG) CD •• Sp. ramosus r•ticutatus ( () .. DAV.& WILL. in DAV. et al.) :0 • - Surcutospha•ridium? tongifurcatum m Trichodinium castan•um (FIRTION) 0 (DEFLANDRE) -0 · X•nascus c•ratioid•s ( - • • • - - DEFLANDRE) CL> - X•nikoon • • - sp. Xiphophoridium alatum & (COOKSON EISENACK) cf- cf- Canning,"a coUirf'ri & I - COOKSON ElSENACK • Cyclon•ph,lium distinctum & - - DEFLANDRE COOKSON BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 37

1977, p. 73). This palynoflora consists of elements of different ages. A relatively large number of Spores and pollen grains from older horizons are, in fact associated with the in situ palynoflora. The rest of the association comprises elements which are too difficult to attribute to either horizon because of their wide stratigraphic distribution. Moreover, the possible redistribution of older sediments had been pointed out by VANGUESTAINE & STREEL, in STRELL et al. (1977). The Normapolles, which only account for about (J) C: 1 % of the palynological content, represent the 0 palynoflora which is obviously in situ . The most ·ua., noticeable amongst them are the genera Trudopo/ (J) lis and Semioculopollis and the main species Q) �a., recognized are Trudopollis nonperfectus, Trudo C: po//is pflugi,� Trudopollis artifex, Trudopollis sp. 1. a., ? Trudopollis sp. 4, Semioculopollis cf. verrucosa, -� "O Semioculopollis cf. sp. A. TscHuov, 1975. Also uco present are lnterporopollenites turgidus, lnterpo I I I I I I I I "O C: ropollenites sp. 1, Fe/deripollenites triangu/us, co ? Hofkeripo//enites sp., Pompeckjoidaepollenites C: I I I I I �a., subhercynicus, Santonipo//is sp. 1. Extrapo//is u co C: sp. 1, AzEMA et al., 1981. Vacuopollis munitus and a., '5 undetermined Normopolles: Normapolle A (Pl. 14. I Q) � CD Fig. 4) and Normapolle B (Pl. 14. Fig. 1 a-b, 2). N a., Although this assemblage is very incomplete. I UJ • :::, the presence especially of the genera Semioculo (!) .S u:::: � pollis, Santonipo//is and Extrapo//is is generally (J) indicative of a Santonian to Lower Campanian age. I I I a., .§ Q) Ol 5.6.2. Beutenaken section co 15 C: Spores and pollen grains are very rare in the � Beutenaken samples, amongst them, a single I 1• I I I• 0 Normapolle specimen in the Beut. 82-7 sample. C: 0 ·5 .0 ·;;: 5.6.3. Cadier en Keer borehole (Fig. 23) en � The two samples taken from the Beutenaken co I I I I u Member at 80-81 m and 78.95-80 m. together with ti ·2 the sample from the Vijlen Member at 75.9-77 m, have yielded material of terrestrial origin. This material represents 30 % of the palynological I I I I 1.J I I I u content at 80-81 m and around 40 % in the other two samples. As in Halembaye. this palynoflora is made up of elements of different ages. The palynoflora which ,:,i C 04J C C E is evidently in situ is represented by a limited ::, E ., .._ Jl O ...... = .. �u11.a: amount of Normapolles. accounting for only 1 % to •II I 3 % of the palynological content : Pseudotrudopol lis pseudoalnus, Pompeckjoidaepollenites sp. 1. , Extratriporopollenites sp. 1, ? Trudopollissp. 3 and Normapolle C in the Beutenaken Member; Trudo- CAMPANIAN MAASTRICHTIA N (pars) STAGES C Ill 'TI HOFKER 's zores ( 1966) w ZEVEN WEGEN M.m�r M•mb•r I LIXHE 1 LAHAYE M.rrt>. Formal lithotypes(FELDER.1975) (X) ::c M•tric seal• r-)> 1"11� LITHOLOGY a, :z: � � J. i: r !i � � J � � � � j J 1"11 � N N SAMPLES � ...... � � � � � :: :: ...... UI "' .. ... 0 ;; � I I I I I I I I I I I G•nus Ocufopollis PFLUG G.nus rrudopollis (PFLUG) KRUTZSCH - - G•nus S•miocufopoffis GOCZAN. KRUTZSCH and PACL TOVA -- rrudopoffis non p•rf.ctus (PFLUG) PFLUG lnt•rporopofl•nit.s turgidus TSCHUDV z Jnt•r poropoll•nit.s sp.1 0 F•ld•ri pofl•nit•s triangu/us KEDVES andHERNGREEN :::0 Normapoll• A ?Hofhripofl•nit•s sp. � rrudopolfis pffugii KEDVES an:I RUSSELL )> ?rrudopoflis sp4 '1J rrudopoffis artifu WEYLAND ant KRIEGER 0 r rrudopoffis sp.1 rrudopofl is sp. 2 r rrl S•miocufopof/is cf. nrrucosa CHRISTOPHER V, S•miocufopolfis cf. sp. A. TSCHUDV 1975 TI Normapoll• B :II Vacuopoffis munitus TSCHUD Y 0 CD Pomp.ckjoidHpoll•nit•s su bt..rcynicus (KRUTZSCH) KRUTZSCH )> Santoni pollis sp.1 U) Elftra pollis sp.1 AZEMA •t al. 1981 � z Bisaccat• poll•n U) • • Afisporit.s grandis (COOKSON) DETTMANN � - Pityosporitu sp. I:, 1· n m Jschyosporitu ps.udor•ticufatus (COUPER) DORING -i N•oraistrickia gristhorp•nsis ( COLIPER)TRALAU • () D•nsoisporitu microrugufatus BRENNER 0 � r S.strosporitu ps.udoafv•ofatus (COUPER) DETTMANN ,:, ;. r Pilosisporitu trichopa pillosus (THIEGART) DELCOURT -,,clSPRU� o • Concavissimisporit.s v•rrucosus DELCOURTInd SPRUMONT � o. Sta plinisporitu caminus (BALME) POCOCK :, .g C•r•bropoll•nitu m.sozoi'cus (COUPER) NILSSON o Ap p lanopsi s dampi•ri (BA.l,.ME) DORING � • Ap planopsis trilobatus DORING !. ui Baculatisporit.s w•llmanii(COUPER) KRUTZSCH - ·--- ;;: Ornam•ntif•r• •chin11t11 (BOLKHOVITINA) BOLKHOVITINA) � Corollina torosa (REISSINGER) CORNET Ind TRAVERSE o. - Corollina m•y•riana (KLAUS) VENKATACHALA Ind GOCZAN St•r•isporitu antiquasporit.s(WILSON �YEBSTER)DETTMANN Gl•ich.niidit.s tri pl•lf (BOLCHOVITINA) DORING Concavissimisporit.s punctatus(DELCOURT lnllSPRUMONT) BRENNER amorphous organic matt•r with coccolith inclusions 8 0 v•�tal c•llular. cuticl•s .•pid•rms 3 o0 cl•ar. fin•ly diviMd matt•r ,,0 .. :, :, -· opaqu. lign•ous partict•s " n CD () cl•ar lign•ous. structur•d woody mat•rial a. :D abundant microfossils UI m 0 r•c•n t contaminations "'O co Total organic carbon f) 1:i FIGURE 22 I Vertical distribution of Spores and pollen grains in the Halembaye section UPPER CAMP. ILOW. MAAS 'Ld UPPER CAMPANIAN LOWER MAASTRICHTIAN STAGES

)> )> OJ aJ HOFKER 's zones (") ZEVEN WEGEN M. V. ZEVEN WEGEN M•mb.r BEUTENAKEN M•mb•r :IJ Formal lithotypes (FELDER, 1975) m I Metric scale 0 LITHOLOGY "U tlL: [... ,/ CD ID ID ID ID � m m ffl C C C C � � �o�oat :jO� � :-i :-i SAMPLES E! 3 g ·g � g � ...CD � z : ... � Trudopollis sp. 3 0 . � Pseud otrudopoll,s pseudoalnus (KRUTZSCH) KR. 3: Pompeckjoid a.po/lenites sp.1 l> (") :t> Elltratriporopollenites sp.1 � s: Trudopollis sp. 2 r � Vacuopollis munitus TSCHUDV z fn j;: Kriegeripollenites retigressus (WEYL. & KR.)K.et HE. Ul � - Bisaccate pollen s: �? :t> -- .. Ill :t> CD Alisporites grand is (COOKSON) DETTMANN :J A (f) ('") -i )>, :IJ rn Sestrosporites pseudoalveolatus (COUPER)DETTM. n 0 C Gleich. triplex (BOLCHOVITINA) DORING ; I ...... -i rn Applanopsis dam pieri (B ALME) DORING � j;: :::0 rn Pilos. trichopapillosus(THIEGART) DELCOURT & SPRU. "8 � z z OJ Cerebr. mesozoicus (COUPER) NILSSON 0 )>, � c.. C -- Cor. torosa (REISSINGER) CORNET & TRAVERSE UI rn :x -0 z '°., 0 0 z lmpardecispora apiverrucata (COUP.) VENK. e,t Ill. Ill., :t> rn -· :IJ Neorais trickia gristhor pensis (C OUPER)TRALAU :J ..UI -< A z UI Cone. rerrucosus DELCOURT & SPRUMONT Ill z rn :J m Q. :t> rn Laricoidites triquetrus LANTZ :IJ :::0 Ster. antiquasporites(Wl.SON et WEBSTER)DE TTM. � Corollina meyeriana (KL.AUS) VENKATA. & GOCZAN :t> :t> (f) -i :IJ :% ,-'.; 0 n Legend � amorphOus organic matter 0 0 I \· .. ! � 3 ., -i 'tJ IC • abundant amorph. org. matt.r with coccolith nclusions • --.. -�. l2iil 0 - common � I, w,getal ce,llular,cuticles, e,piderms :J :J CK:!] ;:;· - present [II] opaque ligneous particles ..:J - rare [II] cr.arlign.ous,structured woody mat.rial UI \::_···II c:::::J re,cent contaminations

�====�;;��======:::;:===:;====:;::::::::TO To tal organic carbone � � �8 ;-.

FIGURE 23 w Vertical distribution of Spores and pollen grains in the Beutenaken and Cadier en Keer sections ( Gleich = Gleiche

pollis sp. 2. Vacuopollis munitus, Kriegeripolleni. tes retigressus and Normapolle D in the Vijlen 6.2. MESOFOSSILS (P.J.F.) Member (Pl. 14. fig. 3, 5-7, 9-11 ). Pompeckjoidaepol The presence of the genus 6.2.1. Introduction lenites (which appears in the Coniacian) and of the genera Trudopollis and Vacuopollis as well as the The Late Cretaceous organoclastic deposits of absence of typical Paleocene genera which are South-Limburg contain a number of very fossilife generally very well represented. suggests a Conia rous bands, which are characterized by the pre cian to Maastrichtian age for this incomplete dominance of a distinctive fossil or group of assemblage. fossils. Since many of these beds serve as regional markers for correlation. they have been named after the dominant fossil in the same. Thus, names such as the "Belemnite Graveyard", "Coprolith 6. - PALAEOECOLOGY Band", "Dentalium Band". "Echinocorys Level"; AND PALAEOENVIRONMENT "Bryozoan Beds", "Hemipneustes Band". and so on, have been established. The fact that these bands can be traced over relatively long distances 6.1. MACROFOSSILS : BELEMNITES (L.A. VDT.) of sometimes twenty to thirty kilometres suggests rather uniform environmental conditions within Belemnites were neritic Cephalopods, probably this part of the Late Cretaceous basin. However, in predating in groups. as recent squids do. In the course of the Campanian and Maastrichtian, general, one can say that belemnite populations, these conditions appear to have varied considera composed of juvenile, adolescent as well as adult bly, as can be deduced from the quite different specimens are found in nearshore. shallow-water dominant fossil groups mentioned above. sedimentary facies, and populations of only adult These variations in the environment have been specimens are found in offshore deposits. Besi investigated systematically in a quantitative study des. Belemnites in offshore deposits are much of the mesofossil content of a large number of rarer than in nearshore deposits (CHRISTENSEN. sections. Mesofossils are all the bioclasts between 1976). In Halembaye and in the Beutenaken area. 1 .0 and 2.5 mm which can be identified as Belemnites occur commonly and all growth stages belonging to one of the major taxa. These include can be found. Regarding their functional morpho both small fossils and fragments of large speci logy and their septa! strength, Belemnites were mens. neritic animals, inhabiting shallow waters (NAEF. 1922; WESTERMANN, 1973). According to JELETZKY In practice, five groups of mesofossils are (1951 ), representatives of the genus Belemnitella distinguished. which can be subdivided into smal are generally associated with a warm-water envi ler groups for more refined correlation purposes : ronment (with e.g. Rudists) and representatives of Foraminifera; the genus Belemnella with a colder-water envi Sponges, Bryozoans, Corals; ronment although the terms "warm" and "cold" Molluscs, Brachiopods; are questionable and must not be exaggerated. as Echinoderms; isotopic measurements suggest (NA1D1N et al., a rest group, including a.o. Arthropods, Serpu 1966). lids, Coproliths, fish remains. This could be an explanation for the disappea Variations in the quantitative distribution of rance of the genus Belemnitella and the appea these groups allow very detailed correlations rance of Be/emnella at the transition of Campa between the different sections in the Late Creta nian-Maastrichtian and the reappearance of Be ceous and Early Tertiary of South-Limburg and lemnitella and the disappearance of Belemnella at surrounding areas, sometimes even over a dis the end of the Lower Maastrichtian. So one may tance of more than one hundred kilometres. The conclude that the Campanian and Maastrichtian method has been applied successfully both for deposits in Limburg were laid down in a near samples obtained from quarries and natural out shore, shallow water depositional regime with crops as well as for rollerbit samples from boreho changing temperature. les (FELDER, 1981, 1982, and in RoBASlYNSKI et al., 1985). For the preparation of the mesofossils, the samples are crushed (insofar as needed), washed CD () :0 m � 0 LLJ ""Cl � LANAYE ENCi NEKAMI VALIENBI.RG WA LEM KS16 KS17 KUNRADE co ::::> 0 HALEMBAYE CADIER en KEER BEUTENAKEN bo ho... le borehol• � VAOENHOVEN HORIZON------I v��---1 1 � ua: t;;

� � ROMONTSBOSCH HORIZON 1.·:·=-�� leii·::.1 �"� u;� () � )> Ill � < � <� z j _;_···- --W15 � ""'� z a: .J':.i l&I = ! W14 Q. : - : � Q. QI · :.:· ..--E15 � ::, ·•· --E16 ·==I I Ell I I U'l =;�.:: ;.-.j--E17 I I ...J I -l ---=- : :0 - I () -E40 :x: -l �· ::::> � Fr.cil CADER •n K. z CD '8c, 0 .r :::�1.' :0 Ochalk z /�� m j! )> z )£:{_1-525 � Limestone :0 rLLJ ;:,'.'.':"'j.". ,1 s j.��--;·-�: � 1� '!!?�!J?�mo :_:.,:::;.:;.-· oc( � Marl,marly � c( U'l 525 :+.�:;:·=.:- -l :0 @Silt,sancl : iISt� 550 /" / N '° :;:;;..;..;./fJ:: () L'·········1-.. fII�"' :x: .. °\ ··,-···( -l l��t:� � Pl!bbles • �·l 550 11+� :""'· 1 I!! •• ) .S!• [�, :- E:JFlint e ....:.::" D � -:.F � Fossil grit · �-�;:·······B·-...... ::::��10lom ....._.:\ ., QJ Glauconlt•

FIGURE 24 Sampling of Campanian-Maastrichtian sections in the South-Limburg for the study of mesofossils and Ostracods � _. � I\) � Y LANA E ENCi !'£KAMI VALIEN!l.1'6 WALEM 1<516 KS17 KUNRADE 1� HALEMBAYE CADIER en l

�-�;.;; r:::;::::::i �I ROMONTSBOSCH HORIZON Ii __ +_ ---Ro��: 111 Z I · - � I- ---1� l••�•I '!'� - z ---·--.1F z 1 UJ � I? ii a: ·=-�:� � :-: l� :. �i :::> I! E a. I � I D : I ,, D I :D C : 1--:-�-,-...-= � 0 CDl> ·�· ::J > U'J � ; c, r BEUTENAKEN �z � U'J a.: f�:::> 88. � LEGEND m '7'='::;···: -I "' ::·:�1-. () ,cu _J L ::/�":'·.; .. 0 i <( :�;;v: Ochalk r -!i j l:::::bvl :··;�T r -;-::·.,· : z .�;. Lim•stone UJ A'm ? :s f;f(·I (ff;} 11 /" ::,�.;·. = 1� ::�:..:..;;:: � Marl,marly c<( _:_ST-. I VAALS <( :>,t·:C1':::;:·: ] A'm ?�I: A'I ) FORMATION fff{_I CJ] Sill,sand NL \ ...••. i}:f1A:1 t�{\; .:?:-.·.·,:: :·,':":".;:: 1:i+fr A'I � Pebbles Wal. Kunr !.: •• .o • . rnir: I •••••• l!! 1ft) E3Flint ENCi . .2 f ::aoCadl: � { ';;£f/J • ·.:;.·::;·::: A'I E �• ••� ·::·· D if .. A'-0 Foram zo,,.s � Fossil grit u. upi,.r part .. . II m. mii:ldl• part �/u:J ...... B ...... :L-b...JOlom.::� .... )_\ Glauconite CD . I. lower part BEN TH IC FORAMINIFERA QJ ():D m 0 "tJ FIGURE 25 co Benthic Foraminifera zones in the Campanian-Maastrichtian of South-Limburg I BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 43 and sieved (meshes used here are 1.0 mm and - Mesofossil ecozone 1 (Vaals Formation). 2.4 mm). Subsequently, the bioclasts are picked Characterized by the predominance of Foramini out under a binocular microscope, separated into fera (Lagenidae), Pelecypods and/or Belemnites. the above mentioned five major groups, and Bryozoans and Serpulids are rare to absent. counted. Finally, the quantitative compostion of Echinoderms become locally abundant towards the mesofossil assemblage in the sample is the top of this zone. calculated . - Mesofossil ecozone 2 (lower part of Gulpen Formation : Zeven Wegen Member to basal part of Vijlen Member). Rapid lateral and verticalchanges 6.2.2. Remarks on mesofossil groups in the quantitative distribution of practically all fossil groups, partly because of repeated rewor Foraminifera. Only the large forms king of material from Vaals Formation and basal ( > 1.0 mm) of this taxon are observed because of part of Gulpen Formation. the size of the bioclasts considered. Two groups - Mesofossil ecozone 3 (upper part of Gu I pen can be distinguished : agglutinated and non-ag Formation : middle Vijlen Member to Lanaye glutinated forms. The latter is composed mainly of Member). Characterized by usually high amounts Lagenidae, Rotaliidae and Orbitoididae. of echinoderm fragments, among which Crinoids - Sponges, Bryozoans and Corals. Sponge abound in the upper part of this zone. Frequently spicules are rare since these usually pass through high numbers of Brachiopods. In the lower portion the sieve. Coral remains are also very rare, since of this zone, mesofossils are very rare. practically all the corals have been dissolved in the - Mesofossil ecozone 4 (lowermost Maas deposits. Therefore, in practice this group consists tricht Formation; "Foraminifera Zone G"). Charac almost entirely of bryozoan remains. terized by predominance of Pelecypods and Be - Molluscs and Brachiopods. These taxa have lemnites, largely reworked from Vaals and/or been taken together, since it is not always easy to Gulpen Formations. distinguish between the fragments of Bivalves and - Mesofossil ecozone 5 (middle portion of Brachiopods. On the other hand, two subgroups Maastricht Formation below Romontsbosch Hori are readily recognized : fragments of belemnite zon). Characterized by predominance of Echino guards and fragments of the prismatic layer of derms, especially Echinoids and Ophiuroids. Lo pelecypod shells. cally high numbers of Serpulids, Bryozans and - Echinoderms. Frequently, a distinction may large non-agglutinated Foraminifera (in so-called be made between Crinoids, Ophiuroids, Asteroids Kunrade facies). Pelecypods and Belemnites are and Echinoids. However, this is not possible for all rare to absent. The lower portion of this zone bears fragments. very low numbers of mesofossils. - Rest group. This heterogeneous group in - Mesofossil ecozone 6 (Maastricht Forma cludes a.o. arthropod remains, Coproliths, Serpu tion, above Romontsbosch Horizon). Characterized lids and fish remains. Only Serpulids tend to be by predominance of Echinoderms (especially common to abundant in some intervals. Echinoids). The lower portion of this zone yields high numbers of Serpulids, whereas non-aggluti nated Foraminifera and Bryozoans tend to abound 6.2.3. Quantitative distribution in the upper half of the zone. Variations in the quantitative distribution of various mesofossil groups and subgroups are shown in Fig. 24 to 31. The correlation lines drawn 6.3. OSTRACODS (M.J.M.B.) on the basis of these quantitative variations match remarkably well the lithostratigraphical and bios 6.3.1. tratigraphical correlations. Therefore, within the Historical review area under consideration, these mesofossil corre Ostracods have been studied from some 180 lations can be regarded as reliable. samples collected from the Vaals to Houthem Comparison of the data on the Fig. 24 to 31 has Formations in ten sections in north-eastern Bel permitted one to· establish a tentative mesofossil gium and South-Limburg (The Netherlands). The ecozonation for the area (Fig. 32). Six major location of these sections and the stratigraphical ecozones may be distinguished, which can be pi>sition of the studied samples is indicated in subdivided into smaller units. Figure 24. :t

� � LANAVE ENCi l'EKAMI VALl KS16 KS17 � 0 HALEMBAYE CADIER en KEER BEUTENAKEN :z: bo,-.hole borehole v��------l YROENHOVEN HORIZON------

AOMONTSBOSCH HORIZON I-��"'.,, ll!i-�_•lt <.....: �·� z,.., j !l I'�·: - 0 a: ..... N Ill !! 8!Ill 11. 1L --' l?�:�-: I :::, ....Q.I!:! , : ' ': ...J ' I: :-n I ::0 => 0 a:, )>

BEUTENAKEN �z (I) 0.::::, 88. � LEGEND m s1.!! -i i;i L () Ochalk 0 ti.1 r !

� lim estone s

[ZJ Marl,marly :;• i N:·········t...."\ CIJ] Silt.sand

� Pebbles nr : � � ( ...... :�;.. : ENCi • r··) De.di« : 6Flint i ···.. :I E :::· D if · � Fossil gril ...... _.\ . ., �}.. ... :.:'.� . a:, �., B t-.b..JO•m 190.,. sp y 50 -qo•,. W Glauconite PORIFERA - BRYOZOA () :0 m 0 "1J FIGURE 26 co Quantitative distribution of Sponges and Bryozoans in the Campanian-Maastrichtian of South-Limburg I a, (") :lJ m 0 "'C LANAYE ENCi !£KAMI VAl..l'ENBLRG WAL EM KS16 KS17 KUNRADE co �z �1 => � � HALEMBAYE CADIER en KEER BEUTENAKEN borehole borehole .... VROENHOVEN HORIZON------� 1

0 co2u

ROMONTSBOSCH HORIZON 1-�;:I', 1-��-·I } Gj�,; I () )> � I� � Zlw z ,·p ; - )>z � l.•I � i �..... I �:i ..a.I� 11�-.- .. � :' (/) :I _J : I :lJ I n::r: :) ---i )> � 2: 0..: z N Q; a, 0---i Nii'§ � � z LEGEND 0 )> C:lJ-< z m ii I� )> :lJ z GIK�17 � � � LIJ� (/) :lJ :�} NL'·······\ ... °\ n::r: ---i r;{:-' � :.. :-· r..., Flint ---i �..• :, D 0:::·· � Fossil grit

�- B �Okm I sp 190·,. Glauconit• .. .. . I) PODA QJ Lf',-,. ... ·····...... � �:� .. .. _\.. MOLLUSCA.,.BRACHI O

FIGURE 27 Quantitative distribution of Molluscs and Brachiopods in the Campanian-Maastrichtian of South-Limburg � (J'I � I j!: LANAYE ENCi I\EKAMI VALKENBLR3 WAL EM KS16 KS17 KUNRADE �- HALEMBAYE CADIER en KEER BEUTENAKEN borehole borehole .... V VROENHOVEN HORIZON------X: ua: z

c(::[ z liz •---· II.I�r :1 a: � "': t :�, �...... I::; �---- . ::> ! � a....J : ' z I :n .. I :0 ,''.i;; � 0 CIJ � => )> 2 f �z � (!) 50 100"1. en 0.: � ::> GI LEGEND m ,"'; .. , -I V) ...J :::::-� () < -��:::_· 0 Ochalk r j _:;q,"':':-, r z �; UJ � Limestone 7 s K�1 51 : " -;�r.:·,�.;·· < ! iz:J Marl,marly < I ft]:·,�.; i -:7"r.;:;· Sill.sand NL ··· ..... LJ g Pebbles Wal. Kunr. \ ... J�l . C' k �c.::· 6Flint . L�. 1 D . , -:···· � Fossil grit urj .... ·····...... �.-�:'.;...... ) .. o �,·· B �Ok� CIJ W Glauconite () PRISMATIC PELECYPODA :0 m 0 -0 FIGURE 28 co Quantitative distribution of Molluscs and Pelecypods in the Campanian-Maastrichtian of South-Limburg 1 OJ (') :::D � m LI.I 0 VE "O LANA ENCi NEKAM I VALMENBIRG WALEM KS16 KS17 KUNRADE co Ii!:� I HALEMBAVE CADIER en KEER BEUTENAKEN I bo,..hole borehole V YROENHOVEN HORIZON t- I ::c: L a:: t;; <� � ROMONTSBOSCH HORIZON �.... u � � 1-��-:"I l•i'�_ak '!I� (') � )> Ill z s:: z� Lul .. l -· -� )> � l ·s0 ( a: 1 z u LIJ LIJ � n.l! � = o �:��.I ::J � �--·- 1' ' ' - 'I � ' ' Cl) ...J �;:;·_ : -t I :::D c=; I -t )> z BEUTENAMEN OJ -qo·,. 0 I sp C BB. IEUT. z ME"8 LEGEND 0 )> -<:::D Ochalk z m )> � Limestone :::D s s:: [ZJMarl,marly � : � Cl) ;; -t N CI] Silt.sand :::D L··· c=; ····· I ·-z -t ... ..i_ � Pebbles (") E3Flint •• ••:U c � .;:;k :U"' ·:::· D t� , .. .. c � Fossil grit ,·1...... ::::; ..... ".:\ I) � B Okm Gtauconite � BELEMNOIDEA W

FIGURE 29 Quantitative distribution of belemnite guards in the Campanian-Maastrichtian of South-Limburg ...... � coJ:i,,

::!!I! .... LA NAVE ENCi IIEKAMI VALICEl'el.R3 WAL EM KS16 KS17 KUNRADE z ::> HALEMBAVE CADIER en KEER BEUTENAKEN � I� - borehole borehole ....-+-��- v��------1 VAOENHOVEN HORIZON------• � z u- 0 a: N t,- 0 l/) i.:;�·1 · �u � -" m�.. o .., \ - � / a::... -- ' - \ � - � 11'1 ,� � "' Mi:::E II.I : z 1 O � � II.I \ U IL II.Il IL a:: 1 :-n I I :0 n 0 �1:i, \ CD )> :;:: ::, en z z �z en � � �:: 1 :, GI m -I n 0 r I r Itz ;., UJ �IKS17 ? u� � :} N L········ \ ... °\ I (;:· 6Flint E < :-" -.::: -·· ; Beul... ·� � 1 . . -,:r: Q Fossil grit 100"1. 50 0 50 100·,. l CD � · B · �°".;, Glauconite () ..... ························"··\. ECHINODERMATA DJ :0 �,· m 0 "CJ FIGURE 30 tO Quantitative distribution of Echinoderms in the Campanian-Maastrichtian of South-Limburg I aJ ("') :II m CJ � "'O LANAVE ENCi tEKAMI VAI..IEMU.RG WA LEM KS16 K517 KUNRADE CD I 5 1 HALEMBAVE CADIER en KEER BEUTENAKEN bor.hole borehole �:I: VROENHOVEN HORIZON------I ... � 20 lil

ROMONTSBOSCH HORIZON 1.::.:-:f\ l•:ear '"� f ("') )> � .7 .. .. . �z !,- )> / - ; -- ...... z � �:�-: : U'l� ' :' -I :II

!' nI -I , :J I )> �� z aJ 0 �� C a: z :::, CJ LEGEND )> :II-< D Chalk z m i )> � i � j :II 1z � Limestone lLI � �17 s 51 : � Marl,marly � !" U'l� � I ·· -I ········; :II CJJ] Slit.sand nI NL -...... -I G Pebbles Wal Kunr 1 ... ·: •:.11. • · :····· E3Flint !E �-.NCi. �Cadlor i 1 -:::· D � Fossil grit IJ IQO't, . ... . sp Glauconile �,u:j . .. 8-···· .... :.�'.;�Okm.. ... _\. I [I] . REST ofMESOFOSS�S

FIGURE 31 Quantitative distribution of the rest of the mesofossils in the Campanian-Maastrichtian of South-Limburg et 50 F. ROBASZYNSKI ET COLL. BCREDP 9 (1985)

If) z U) 0 � Ill� 0 u 0 ,- � � ::c: If) u ...I

KASTANJELAAN 2 BOREHOLE a: ,- < 0:: J: � i: u Q.. w fr w 0 0::

FIGURE 32 Synthetic quantitative distribution of mesofossils in Campanian-Maastrichtian of South-Limburg and definition of the six mesofossils ecozones

The study of Late Cretaceous and Early Tertiary difference in the species diversity observed in the Ostracods from this area started already halfway various stratigraphic intervals. Species diversity is through the last century (BosouET. 1847. 1854). low in the Gulpen Formation (beween 20 and 36 More detailed investigations have been carried out species) and high in the Maastricht Formation in this century (VAN VEEN : 23 publications between (between 75 and 125 species). This suggests 1932 and 1937; Drnoo. 1966; RoMEIN et al.. 1977). important changes in the palaeoenvironmental Almost 250 species have been describ-ed thus far. conditions. Practically all species had been obtained from the These variations in the palaeoenvironment may Gulpen. Maastricht or Houthem Formations. Only also be deduced from a quantitative investigation a few species from the Vaals Formation have been on the assemblages. as carried out for this paper. described by Drnoo (1966). However. the latter For this purpose two purely artificial groups of data must be considered as incomplete since only Ostracods have been distinguished : more or less very few samples had been studied. Finally, some smooth-shelled forms (Plate 19) and ornamented remarks on the palaeoecology of the Ostracods (Plates 20 to 22) ones. This was done on the have been published by BLESS et al. (1983) and in assumption thr1t many smooth-shelled Ostracods ROBASZYNSKI et al. (1985). have a rather fragile carapace compared to that of ornamented ones. and that smooth-shelled Ostra 6.3.2. Palaeoecological value cods might therefore be indicative for low-energy and/or relatively deep environments. whereas A review of the species list published by Drnoo ornamented Ostracods might show a preference (1966. table 6) readily learns that there is a marked for high-energy and relatively shallow facies. Of BCREDP 9 (1-985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 51 course, it was realized that this assumption is an whereas the ecozones 7 to 15 are commented in oversimplification, and that the terms "low and a more generalized way. high energy", "shallow" and "deep" have only a - Ecozone 1 comparative meaning. For example, the term Roughly corresponding to the lower and middle "deep" is used here in the sense of "less shallow" Vaals Formation. Ornamented Ostracods are pre and reversely the term "shallow" is meant as "less deep", without fixing any exact figure to the dominant in many samples (up to 82 % ornamen boundary between shallow and deep and even ted forms in Beut. 82-8). but occasionally, there accepting that this boundary may be flexible. occurs a predominance of smooth-shelled speci mens. Characteristic are Veenia, Cythereis, Ptery The group of smooth-shelled Ostracods as gocythere whereas Pterygocythereis, Curfsina and defined here comprises the genera Cypridina, Cytherella are common. Sometimes high numbers Cytherella, Bairdia, Macrocypris, "Paracypris ", of Bairdia or Asciocythere. Xestoleberis, Asciocythere, Clithrocytheridea, Pa rataxodonta, Aequacytheridea, Veenidea, Kalypto - Ecozone2 valva, Krithe, Globoleberis, Sphaeroleberis and Roughly corresponding to the upper Vaals Tumidoleberis. The latter three genera frequently Formation. Predominance of smooth-shelled Os show a finely striated ornament and an inflated, tracods (between 80 and 100%), especially Cythe somewhat overhanging latero-ventral portion of rella and Asciocythere. Commonly some speci the valves. Therefore, these might as well have mens of Veenia. Pterygocythere and Cythereis. been included in the group of ornamented Ostra - Ecozone3 cods. All the other genera ( Cytherelloidea and a Corresponding to the base of the Zeven Wegen large number of genera assigned to the Cythera Member. Predominance of smooth-shelled Ostra cea by DERoo. 1966), have been considered as cods (Bairdia. Krithe), but relatively high numbers ornamented, even if their carapaces may be (prac of ornamented Ostracods (up to 30 %), notably tically) smooth (e.g. some species of Kikliocythere Cytherel/oidea and Bythoceratina. and Mosaeleberis). - Ecozone4 Subsequently, the number of individuals be longing to one of these two groups has been Corresponding to the middle and upper portion counted. In each sample a minimum of 25 ostra of Zeven Wegen Member and base of Beutenaken Member. Predominance of smooth-shelled Cythe cod specimens were counted (no distinction was rella (in Halembaye samples) or Bairdia (in Beute made between single valves and complete cara naken and Cadier en Keer samples). Regularly paces). But frequently up to 50. and occasionally some specimens of Cytherelloidea and Bythocera over one hundred specimens were counted. If the tina, whereas Mosae/eberis rutoti occurs in several number of specimens was below 25, the countings samples of the Zeven Wegen Member. of two successive samples have been combined into one larger sample interval. It was observed - Ecozone5 that smooth-shelled individuals usually predomi Corresponding to the middle portion of Beute nate over ornamented forms (except for the lower naken Member. Predominance of smooth-shelled and middle Vaals Formation and occasionally in genera Asciocythere and Bairdia, and relatively the Maastricht Formation. where ornamented high numbers (30 % to 37 %) of ornamented forms Ostracods may be predominant). Therefore. a (notably Cytherelloidea. Aversovalva. Bythocera practical cut-off value of 80 % smooth-shelled tina, Schizocythere. Curfsina and Eucytherura individuals in a sample was accepted for the dorsotuberculata). distinction between "smooth" and "ornamented" assemblages. This approach allowed the recogni - Ecozone 6 tion of fifteen assemblage zones or ecozones Corresponding to the top of Beutenaken Mem which can be traced from one section into the ber. Vijlen. Lixhe 1-2-3 Members. and the lower other (Fig. 33). This suggests extremely uniform portion of Lanaye Member. A predominance of ecological conditions within the basin. ornamented Cytherella. Regularly low numbers of Krithe and Aversovalva. Isolated specimens of Bythoceratina and Eucytherura dorsotuberculata in Vijlen Member. 6.3.3. Definition of ostracod ecozones The ecozones 7 to 11 show characteristic For the scope of this report, short characteris off-lap (zone 7) and on-lap (zones 8 to 11) pheno tics of the ecozones 1 to 6 are presented below, mena. U1 N

Y LAHA E ENCi IIEKAMI VALl'Eel.RG WAL EM KS16 KS17 KUNRADE � BEUTENAKEN borehole borehole i I �1 HALEMBAVE CADIER en KEER ; YROENHOYEN HORIZON------V OSTRACOD U>' ·-· ECOZOIES

0 H0 IZ N ...... · · .. ·· ...... jij�'. ROMONTSBOSCH R O r:·:-:-t...... 1.--.:.1 ...... � ...... ,;;.�U, z � ...... , ! 10 j 1 ---- - UJ . 9 ·1: ...... - .... ,�_ :" °' I "'.'7".'-7 ..: .. I I L.

_J ,, !I : :D 0 aJ :l }> Vl z Vl� m LEGEND -I () 0 Ochalk r !

z � Limestone 17 � ) �1 � Marl,marly 1 : ' 0 } �I Silt.sand ···· [J2ill NL ····--c .... \ � Pebbles

§Flint 0 G.:, Li =--...2:'" • Fr FROIDMONT HORIZON < �, - ' L LOEN HORIZON a.u,. · -,� � Fossil grit . r . . �· 1 . . � . . � · ...... HE ...... _• • •• \• 10 e ��!�og .t�fMBLAGE ; + ORNAMENTED OSTRACOD ASSEMBLAGE aJ �km Glauconite () � B 1-13 OSTRACOO ECOZONES OSTRACODA [I] :D -.... BOUNDARY BETWEEN OSTRACOOS ECOZONES m 0 "'tl FIGURE 33 (0 Distribution of the thirteen ostracod ecozones in the Campanian-Maastrichtian of South-Limburg I BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 53

Of special importance is the succession of the may be related to the fact that the Maastricht area assemblage zones 10 to 13. which has been was within the reach of the Boreal realm during recognized in the ENCi. Nekami and Kunrade the Campanian and large part of the Maastrichtian. sections. and partly also in the Valkenburg section and became a part of the Tethyan Province at the (zones 10 to 12). This succession confirms the end of the Maastrichtian (deposition of the correlation of the "Koraalkalk van Kunraad" Hori "type-Maastrichtian" of DUMONT. 1849). zon in the upper portion of the Kunrade section with the Romonstbosch Horizon in the ENCi and Nekami sections (FELDER. 1977). and is convincing 6.3.5. Palaeoecological implications evidence for the suggestion by FELDER (1977) that CLARKE (1983) suggested an increased tempera the Kunrade Chalk corresponds to the lower ture for a.o. the Lower Maastrichtian of Hemmer portion of the Maastricht Formation (Mb). insofar (Federal Republic of Germany) because of a.o.· the as exposed at the ENCi. However. this is a increased number of species and individuals of problem that deserves a more detailed discussion the "warm-water" genus Cytherelloidea in the beyond this paper. uppermost Campanian and Lower Maastrichtian. The Halembaye section clearly shows the However. this increase in the number of species is presence of important gaps at the position of the not spectacular (usually from two to incidentally Loen Horizon and Froidmont Horizon. where four). Moreover. the high numbers of valves per marked environmental changes took place in other 100 g sediment (between 50 and 170) correspond sections. Also it should be noticed that the ostra to low numbers of species (two). Therefore. this cod content of the Halembaye section is not argument is considered as insufficient for accep necessarily a standard one for the basin. This may ting the hypothesis of an increased sea-water be deduced. for example. from the observation temperature during that period. On the other hand. that lateral variations occur in e.g. the ecozone 4. CLARKE'ssuggestion that the minimum temperature where the genus Cythere/la predominates at of the sea-water in northwestern Europe was 10<>C Halembaye and the genus Bairdia at Cadier en because of the presence of a.o. the "warm-water" Keer and Beutenaken. genus Cytherelloidea seems valid. Such tempera tures are not restricted however to the seas 6.3.4. Species diversity between 40<> southern and northern latitudes. These may occur also further to the North than to Species diversity and the number of genera are the South because of warm oceanic currents. such highest in the ecozones 1. 3. 5 and 7. where the as the recent Gulf Stream. percentage of smooth-shelled Ostracods is less than 80 %. The number of genera and species is lower within the ecozones 2. 4 and 6. Similar observations have been made for the Maastricht 6.4. SPORES AND POLLEN GRAINS AND ORGANIC and Houthem Formations. MATTER (O.L.) This suggests that ostracod species invaded the basin during periods of optimal ecological Terrigeneous organic supplies are negligible in conditions. when the mega-environment was rela the Gulpen Formation at Halembaye and at Beute tively shallow and the water energy level- not too naken : Spores and pollen grains are very rare and low (presumably above wave base and well-aera the organic carbon content very low. suggesting a ted). When the mega-environment became deeper greater distance from the shore. These supplies in subsequent periods. the number of species are significantly higher in the Vaals Formation at decreased. apparently because of a less suited Halembaye and in the Beutenaken Member and facies. Such a rhythmic variation in the composi Vijlen Member at Cadier en Keer : Spores and tion of the ostracod assemblages suggests that pollen grains are much more numerous and the the appearance and disappearance of the ostra organic content higher. These observations are cod species is strongly facies-controlled. There indicative of more near-shore conditions. underli fore. the (eco-)stratigraphical ranges of the Ostra ned also by the presence of autochthonous amor cods in this area are not necessarily the same as phous organic matter with coccolith inclusions. in other regions. The presence of autochthonous organic matter is The relatively low number of ostracod species evidence of an environment of deposition which in the Vaals and Gulpen Formations against the ,favours its good preservation. i.e. poorly oxygena high species diversity in the Maastricht Formation ted conditions at depth. 54 F. ROBASlYNSKI ET COLL BCREDP 9 (1985)

As it was expressed in the biostratigraphieo sus. Cerebropollenites mesozoicus. lmpardecis chapter. a redistribution of older sediments is pora apiverrucata. Concavissimisporites verruco emphasized by the occurrence of reworked Spores sus (Pl. 15). and pollen grains. As in Halembaye. the presence of Neoraistric kia gristhorpensis and of Corollina meyeriana indi cates the resedimentation of deposits which are 6.4.1. Reworked Spores and pollen grains Bathonian-Bajocian and Upper Trias to Lias in age. The bisaccate pollen grains represent 30 to A reworking of deposits is revealed at Halem 40 % of the material of terrestrial origin: amongst baye quarry (Fig. 23) by the presence of quite a lot these. Alisporites grandis. Their varied colouring of Spores and pollen grains. Most of the reworked shows that. just like those in Halembaye, they species have a limited stratigraphic extension come from different horizons. which. for the most part. is common to them all. The longest of the stratigraphic interval stretches As in Halembaye, the quite dark Circumpolles from the Kimmeridgian to the Cenomanian and the pollen are probably all reworked from older levels. shortest one is from the Hauterivian to the Aptian . Cerebropollenites mesozoicus Pilosisporites tri 6.4.2. Organic matter chopapillosus. Concavissimisporites verrucosus. Concavissimisporites punctatus. Applanopsis The highest organic carbon content has been dampien� Applanopsis trilobatus. Sestrosporites found in the Vaals Formation at Halembaye quarry pseudoalveolatus. Baculatisporites wellmami (Fig. 22) although even here it remains low: TOC Densoisporites microrugulatus. Ornamentifera is in the order of 0.45 % (TOC : Total Organic echinata. Gleicheniidites triplex. lschyosporites Carbon). The terrigeneous supplies are more pseudoreticulatus (Pl. 15). numerous here than in the rest of the section; this Some species such as Corollina torosa (Pl. 15) is indicated by the presence of terrestrial micro have a slightly longer stratigraphic extension. flora, even though in a relatively limited quantity. ranging from the Upper Trias to the Cretaceous. The organic matter comprises half amorphous and half ligneous matter. The amorphous matter Furthermore, the presence of Neoraistrickia contains many coccolith inclusions which attest to gristhorpensis (Pl. 15) restricted to the Bajocian its algal origin (Pl. 14. fig. 12-13) and therefore to Bathonian and Corollina meyeriana (Pl. 15) known from the Upper Trias to the Lias. indicates the its autochthonous nature. whereas the ligneous resedimentation of even older Jurassic deposits. material comes from the mainland. In the Gulpen Formation. the organic carbon content is very low The bisaccate pollen grains are relatively nume TOC < 0. 1 %. The organic deposits are. therefore, rous. accounting for about half the material of negligible and the palynofacies are not very repre terrestrial origin : these pollens include Alisporites sentative : they consist of ligneous material asso grandis and Pityosporites sp. Their varying colou ciated with a small amount of amorphous matter ring suggests that they probably have been deri below the Froidmont Horizon. In the Lixhe Mem ved from different horizons and that some of the ber. most of the palynofacies are made up of quite light ones are in situ. dinoflagellate cysts. The relatively dark colour of the Circumpolles Organic carbon content is very low in all the pollen grains with Corollina meyeriana and Corol samples of the Beutenaken section : TOC < 0,1 %. lina torosasuggests that they have all been rewor The organic deposits are negligible and the paly ked from older levels. nofacies are not very representative. They show The samples taken along Beutenaken section mixed amorphous-humic facies that are generally (Fig. 23) contain very few Spores and pollen highly contaminated by subactual pollutions. grains. A few reworked elements including Corol At Cadier en Keer, organic carbon content is lina torosa in the Beut. 82-2 and Beut. 82-1 low in the three samples : the TOC varies from 0.15 samples. can be noted. to 0, 12 %. The presence of terrestrial microflora Reworkings of the same type as those obser reflects the terrigeneous supplies which. however. ved in the Vaals Formation at Halembaye, are remain limited. The organic matter consists mainly visible at Cadier en Keer (Fig. 23) in the Beutena of amorphous material combined with a small ken Member and in the Vijlen Member: Sestros quantity of opaque ligneous material. All of the pon'tes pseudoalveolatus. Gleicheniidites triplex. amorphous matter in the Vijlen Member and a part Applanopsis dampieri, Pilosisporites trichopapillo- of it in the Beutenaken Member contains coccolith OJ () :D m 0 ""O co

(83MA) (72MA) (65MA) j CAM PANIAN LOIi. MAASTR. UPPE R MAASTRICHTIAN :VAALS FM. GULPEN FM. MAASTRICHT FM. Upp.r () s::)> HALEMBAVE � ENCi z )>z BEUTENAKEN � KS16-KS17 � (/) -i PALAEOGEO· BorNI :D { n GRAPHY T•thy., I \___ -i )> ·Shallow" z WATER DEPTH { CD "DNP" 0 C NNrshor• z DISTANCE 0 { TO SHORE Oftshor. )> :D-< z ·warm" m TEMPERAT\R { "T•ms-rat•" )> I :D "Cold• (.ways i.10"C) '--�__,I s:: )> WATER { High )> \•(.nul flows) (/) EIIEAGY /\* -i Low ft tJt..J'(J(_f n:D I { Soft SUBSTRATE -i Firm <· hardground)� )J -�

FIGURE 34 Main variations of palaeoecological conditions in the Campanian-Maastrichtian of South-Limburg

u, u, 56 F. ROBASlYNSKI ET COLL. BCREDP 9 (1985) inclusions and is, therefore, of algal origin (Pl. 14, double-keeled and single-keeled more below. If fig. 12-13). we follow this interpretation. the occurrence of only globular or slightly double-keeled forms in the Vaals Formation involves a shallow marine 6.5. FORAMINIFERA environment. In the basal glauconious white chalk of the Zeven Wegen Member. rare Archaeoglobigerina 6.5.2. Benthic Foraminifera (J.P.M.Th.M.) are accompanied by some Globotruncana of the A comparison at the family level of benthic double-keeled "area group" which indicate a less Foraminifera. from the Campanian and Maastrich shallow marine environment. tian deposits in the Maastricht area with those of In the calcilutites and calcarenites of the Beute modern seas suggests that the water depth varied naken. Vijlen and Lixhe Members. Globotrunca between 40 and 150 m during the sedimentation of nids are more diversified. but small and globular the Gulpen Formation and between O and 40 m forms are dominant. In addition to Archaeoglobi during the sedimentation of the upper Maastricht gerina and Globigerinelloides, specimens of dou Formation (VILLAIN. 1977). ble-keeled forms as Globotruncana area and in A similar comparison suggests a relatively termediate forms of Globotruncana arca-rosetta "cold" water temperature during the deposition of were found with very rare single-keeled forms the calcilutites of the Gulpen Formation. whereas such as Globotruncanita stuartiformis. Should the the water was warm (20-25°C) during the sedimen latter keeled species be abundant. they would tation of the highest ("Md") Maastricht Formation suggest a deep water environment. but their (VILLAIN, 1977). scarcity suggests that their presence is more probably the result of marine currents which Important differences exist in the qualitative transported them into a relatively shallow marine and quantitative composition of the Foraminifera environment. assemblages from the Zeven Wegen Member in the Halembaye and Beutenaken sections. These may be due to selective preservation, to the fact that only a few spot samples have been compared, 6.6. NANNOPLANKTON AND DINOFLAGELLATES or to local differences in the palaeoenvironment. (H.M., J.-C.F.) The qualitative composition of the Foraminifera assemblages from the Beutenaken Member in the Cadier en Keer and Beutenaken sections is very A great part of the nannoflora from Limburg similar. However, there are differences in the calcilutites and calcarenites belongs to the Boreal quantitative distribution of species. For example. province characterized by the scarcity or the Gavelinopsis voltziana and Eponides beisseli are absence of index species known in Tethyan common in the Beutenaken section, whereas Cibi province as in Tunisia or Charentes. as Ouadrum cides subbosqueti and Gaudryina cretacea are gothicum, Ouadrum trifidum and Ceratolithoides amongst the most frequent forms in Cadier en aculeus. On the other hand. the rarity of these Keer. species is compensated by the abundance of Therefore, it seems premature to use the Arkhangelskiella, Reinhardtites anthophorus which quantitative distribution of benthic Foraminifera for then evolves into Reinhardtites levis and also the a palaeoecological interpretation. increasing of Eiffellithus turriseiffeli. E. gorkae, Lithraphidites carnio/ensis and Prediscosphaera cretacea. All these nannofossils are generally 6.5.2. Planktonic Foraminifera and sea-depth predominant in the high latitudes ( > 35-4Qo) as (F.R.) noticed by THIERSTEIN (1976). Moreover. this author In the Vaals Formation. only some globular and considered that Lucianorhabdus cayeuxi and Pha slightly double-keeled forms were recorded as. for nulites obscurus were two "hemipelagic" species example. specimens belonging to the genus Ar of high latitudes and that the presence of Kampt chaeoglobigerina and one specimen of G/obotrun nerius magnificus could be interpreted as an cana cf. bulloides. According to HART (1980) and indicator of nearshore environment. CARON (1983). the speciation of Globotruncanids The good preservation and the clean aspect of has been controlled partly by the sea-depth. As all Coccoliths observed in the samples studied the sea-depth increases. globular forms become give no evidence for a reworking of the nannoflora. BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 57 Thus. the presence of numerous Nannoplank 6.7.2. Relative water depth ton and Dinoflagellates indicates that calcilutites and calcarenites from Limburg were deposited in It is suggested that all the Late Cretaceous an open marine environment. deposits in the Maastricht area have been laid down on the marine shelf. This points to a maximum water depth of 200 to 400 m. In practice. 6.7. PALAEOECOLOGICAL SYNTHESIS however, the water depth in this area will have (M.J.M.B., P.J.F., J.P.M.Th.M.) been considerably less than these maximum figu res. probably with an average of 40 to 100 m. The terminology used for describing depositio According to ALBERS (1976), the deposits of the nal environments is not quite uniform. For exam Vaals Formation suggest sedimentation in a shal ple, an ecological niche at 150 m below sea-level low sea. par\ly within the reach of wave action. remains a problem. because the exact depth of the This means within a depth of say 40 to 50 m. depostion of many marine shelf sediments is VILLAIN (1977) suggested a water depth of some virtually unknown. Therefore. one should keep in 80-100 m for the Zeven Wegen. Vijlen and Lixhe mind that terms as deep and shallow, cold and Members of the Gulpen Formation. This interpreta warm, of offshore and nearshore are used here in tion was based on the association of benthic a comparative way, and not in an absolute one. Foraminifera occurring in the calcil.utites. calcisilti tes and calcarenites of this Formation. Relatively high numbers of ornamented Ostra 6.7.1. Palaeogeographical influences cods are frequent in the deposits of the Vaals Formation and in the upper portion of the Maas tricht Formation. These are relatively rare in the The Campanian and Maastrichtian deposits of Gulpen Formation and lower portion of the the Maastricht area reflect influences of the Boreal Maastricht Formation. Presumably, high numbers and the Tethyan realms. of ornamented Ostracods are characteristic for Boreal conditions prevailed during deposition relatively shallow environments, whereas assem of the Vaals. Gulpen and the lower part of the blages characterized by more than 80 % smooth Maastricht Formations. These are characterized by shelled specimens are indicative comparably for relatively low numbers of macrofossils, showing a more deep marine facies (BLESS, 1983; BLESS et al., comparatively low diversity. Bivalves and Cepha 1983). lopods frequently dominate. The frequent occurrence of the ostracod genus During the Upper Maastrichtian the number of Cytherelloidea in the Zeven Wegen Member and in fossils and of taxa increases rather rapidly in the the lower portion of the Vijlen Member may be upper portion of deposits characterized by benthic considered as an argument for a maximum water Foraminifera belonging to HoFKrn's zones H-1 and depth of 200 m. The optimal distribution of these J. Presumably, many of these taxa are conspecific Ostracods is in seas with a maximum depth of or closely related to those considered characteris 100 m (KozuR. 1972; LIEBAU, 1976). tic of the Tethyan realm. Therefore. it seems reasonable to accept that VILLAIN (1977) argued that a migration of Medi the Gulpen Formation has been deposited in a terranean Foraminifera from the Aquitaine into the shelf sea of some 80 to 100 m depth. Maastricht area (as suggested by DEROO, 1966) at The abundance of broken fossils, and of a.o. the end of the "Mb" (in upper part of foraminifera Corals. Bryozoans, Serpulids and calcareous Algae zones H-1 and J) is not very likely. However, it in the upper portion of the Maastricht Formation is cannot be denied that a number of characteristic considered as an indication for a very shallow Tethyan Foraminifera (a.o. Siderolites and Orbitoi marine shelf with a maximum depth of less than dea). the "warm-water" Serpulid Sc/erostyla mo say 50 m. sae (BRONN) as well as the first Rudists (which are common in many shallow-marine Tethyan depo sits) appear in this region at the end of the Mb. 6.7.3. Relative distance to the shore line This means that the deposits of Halembaye, The regular occurrence of silicified wood and Beutenaken. Cadier en Keer and Bovenste Bosch other land-derived macrofloral remains in the have been laid down under prevailing Boreal Vaals Formation and in the upper portion of the conditions. 'Maastricht Formation suggests that these sedi- 58 F. ROBASZVNSKI ET COLL. BCREDP 9 (1985) ments have been deposited in a more nearshore. ments of prismatic Bivalves possibly belonging to environment than those of the Gulpen Formation some lnoceramid. the relatively low diversity in the and lower part of the Maastricht Formation, where Dinoflagellates. and the practical absence of macrofloral fossils are practically absent. Bryozoans and Crinoids. Moreover. the occurrence The significantly higher quantity of organic of the ostracod genus Cytherelloidea in the Beute terrigeneous supplies in the Vaals Formation as naken Member suggests that the temperature was compared with the Gulpen Formation at Halem not lower than about 1QoC.This supposition should baye and Beutenaken is indicative of a more be corroborated by oxygen isotope analyses in the nearshore environment. Similar conditions are future. observed at Cadier en Keer. in the Beutenaken Member and in the Vijlen Member. 6.7.5. Water energy In contrast. the very slight terrigeneous influen The water energy level must have been relati ces observed in the Gulpen Formation at Halem vely high during the deposition of the Vaals and baye and at Beutenaken suggests a greater dis Maastricht Formations and relatively low during tance from the shore line. the deposition of the Gulpen Formation. The latter The presence of washed-in glquconite and is characterized by very fine-grained sediments reworked Spores and Pollen grains in some levels (calcilutites. calcisiltites to calcarenites). whereas at the very base of a.o. the Zeven Wegen, Beute the former mainly consist of medium- to coarse naken and Vijlen Members of the Gulpen Forma grained sediments (sands of the Vaals Formation tion might be interpreted by accepting mud flows and calcisiltites to calcarenites of the Maastricht from the very shallow nearshore into the some Formation). what deeper offshore shelf. The medium- to coarse-grained glauconitic chalk bands at the base of a.o. the Zeven Wegen. 6.7.4. Relative temperature Beutenaken and Vijlen Members of the Gulpen Formation are here interpreted as mud flows from Accepting the hypothesis that Tethyan currents a very shallow into a somewhat deeper environ reached the Maastricht area somewhere during ment (thickness less than 10-20 cm). the Upper Maastrichtian (in the upper portion of HoFKrn's Foraminifera zones H-1 and J) we may believe that the sea water temperature was higher 6.7.6. Substrate during the deposition of the upper portion of the Maastricht Formation than in the period before The substrate of the Campanian and Maastrich when this area was predominated by Boreal tian seas in the Maastricht area has been usually conditions. soft and/or muddy. This is suggested by the large number of burrowing organisms (e.g. irregular This does not mean that the sea in the Boreal Echinoids. Ostracods such as Cytherella and Cy realm was (everywhere) a cold one. Living species therelloidea. Bivalves such as Pinna, Lobsters of of the ostracod genus Cytherelloidea (frequently Ca/ianassa-type). A more firm substrate developed occurring in the Vaals and lower half of the Gulpen from time to time during the Upper Maastrichtian Formations) prefer a minimum bottom tempera (hardgrounds), possibly during intervals of (practi ture of the sea water of 1QoC (CLARKE, 1982). This cally) no sedimentation and sometimes with ero genus is also common in the Lower Maastrichtian sive marine currents. Such hardgrounds are cha of Rugen and Hemmoor (HERRIG, 1966; CLARKE, racterised by the frequent occurrence of vertical 1983). This suggests that the sea water tempera burrows and a very fossiliferous layer on top. The ture of the Boreal realm in northwestern Europe erosion horizons at the base of a.o. the Zeven may have been relatively warm or temperate rather Wegen. Beutenaken and Vijlen Members of the than cold. Gulpen Formation may be explained as a result of A transitory drop of the sea water temperature turbidity currents and mud flows. These might also in the Maastricht area may have occurred during have transported the medium- to coarse-grained the Lower Maastrichtian (Beutenaken Member). chalk and glauconite into the area. The fossil assemblages of the Beutenaken Mem ber are distinguished from those of the underlying 6.7.7. Conclusions Zeven Wegen and overlying Vijlen deposits by the presence of the Cephalopods Belemnella and the The mean palaeoenvironmental conditions in absence of Belemnitella. the abundance of frag- the Maastricht area during the Campanian and BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 59

Maastrichtian are summarized in Fig. 34. Apparen Only the type-Maastrichtian presents some Te tly, many ecological factors controlling the fauna! thyan characteristics. for example the presence of assemblages at the Campanian-Maastrichtian Rudists (rare) and of large benthic Foraminifera boundary did not change so much. The water (rare levels but with numerous Orbitoides, Lepi depth (80- 100m). distance to the shore line dorbitoides. Ompha/ocyclus. Hellenocyclina. Side (offshore) and water energy (low) remained the rolites; et. V1LLAIN, 1977). same. But there seems to have been a critical In each palaeontological group, several species change in the temperature. although the overall seem to be particularly significant, whether by boreal conditions remained constant. These re their extinction or by their appearance. The vertical sult a.o. in the transitory disappearance of the distribution of the main species is given in Fig. 35 belemnite genus Belemnitella (that returned at the (Remark: with regard to the preliminary results base of the Vijlen Member) and the temporary presented at the "Senonian" Colloquium in Mar appearance of the genus Belemnella. seille - cf RoBAS2YNSKI et al., 1985 - the study of A turbidity current of mud flow at the base of new samples and of new sections allowed one to the Beutenaken Member has faded out the original explain or to modify the distribution of some taxa). boundary between the Campanian and the Maas trichtian. This current eroded the top of the • Belemnites underlying Zeven Wegen Member and deposited The species Belemnella lanceolata inflata ap a layer of varying thickness (some cm to 1 or 2 dm) pears in the Beutenaken Member and is present in with a mixture of reworked sediments and fossils situ only in this member. The Beutenaken Member of the Vaals Formation and the Zeven Wegen is also capped with a level containing reworked Member and (equally reworked) sediments and Belemnella "occidentalis". Thus. the Beutenaken fossils of the basal Beutenaken Member. chalk Member. of some metres thick. represents a part of the Lower Maastrichtian (as this substage is defined in the Bore al realm, cf. SCHULZ et al., 1984). The Upper Maastrichtian begins in the 7. - CONCLUSIONS Vijlen Member with the appearance of Belemni tella junior.

The type-Maastrichtian of DuMONT (1849) is • Foraminifera exposed in Limburg, especially in the ENCi quarry In the Lower Maastrichtian Beutenaken Mem located south of Maastricht. It is represented by ber appears the small benthic Foraminifera spe- , the calcarenitic Maastricht Formation lying on a cies Bolivinoides australis which is characterized glauconious bed named Ma by UHLENBROEK (1905. by a number of pustules on the last chamber 1912). between 4 and 5. Several other benthic species But since ARKHANGELSKY (1912) and JELETZKY also appear in the Lower Maastrichtian as Neofla (1951 ). an agreement came to lower the base of bellina praereticulata and Eponides beisseli. The the Maastrichtian. A Maastrichtian stage begin incoming of these species seems to be useful in ning. in the Boreal realm. with the appearance of the chalky facies of the whole Boreal realm. Very Belemnella lanceolata was officialy proposed by rare planktonic Foraminifera are represented es 81RKELUND et al. (1984) during the tenure of the pecially by specimens of Globotruncana gr. area, International Geological Congress of Moscou. but they are not so numerous and their morpho 1984. This proposal is followed herein. logy is not so characteristic enough to be used as Taking into account the definition of this boun stratigraphical markers. dary between Campanian and Maastrichtian sta ges. the intention of this work was to know what • Nannoplankton were the vertical distributions of various palaeonto In the Beutenaken Member appear Lithraphidi logical groups on both sides of this boundary in tes praequadratus and Reinhardtites levis whe the type-Maastrichtian region. In this way, a series reas, above, Reinhardtites anthophorus, Broinso of samples were studied from the Vaals Formation nia parca constricta and Eiffellithus eximius are still and mainly from the Gulpen Formation where this present and extinct in the Upper Maastrichtian Campanian-Maastrichtian boundary is present. Vijlen Member. We should recall that both these two Forma Lucianorhabdus cayeuxi linked with Phanulites tions were deposited in a Boreal environment. 'obscurus extinct higher in the Lixhe 1 Member and LOW. CAMP. UPPER CAMPANIAN UPPER MAASTRICHTIAN : 0) (/) STAGES 0 < L.MA. n :r-::J � l> a, O "1 "TI I HOF KER 1966 smectite craie bla nch• ;:�:. craie gr is e craie tigree , in CALEMBERT 1956 () m 1g;::�iire: ::::,-c'," g ;:i. VAALS Form. ZEVEN WEGEN M•mber VULENMemb LIXHE Members LANAVE: LITHOTVPES Q) 1 I 2 I 3 (oar s) "' I 1 and FELDER, 1975 :E 1 I � 6 i' � Ill c :i::� � )!! .,.. :x;'i ; � �... 111 ! 1 HORIZONS • m� "1 Z l'I i!': �� ;;\ I ::I: N zi z !!I f• R mm Ill ,.. • r ;:i. "' - )> < � o :i: '" 17 :;; -'° • C1) < o �� :: ., nm rn ��- 111 Zi .- � ::z: � 1111'1 :: j; .:I � : _.., ! ; � I ; . l>ITI � ui � � -4 I'! 0 3 � .. :i:: , • 1 I cc m Q) en - · • 1 • 1 • , • . z.. 1I•,', 1 -: • , • , • 1 , 1 � ( '1 1 � Q. I 1• , q 1 ,•1.,• • •IJ'I =tJITI < 1 ·' ' ::�-�·.'•�?!; '." �!· t,1.f ;f.:l:;::t'f','.J.l:i;;:; S'':l'1 /. )> {': •.' 1�J�'t1�,·�¥',: ,C:-/"I ��o·=:- .' }\: - § LITHOLOGY -,,,Z ITI..... mm:·:I I •• \{ 1 I Ill... I I I l�I 11 I I.---'• • ' .f •' ' ::::,::,:: Q) - 'I')> ::Jo· ITI ga- ::J Z :I: ::t: ::t: I I :I: ::t: ::t: � ::t:� :: �� ::t: ::t: - :I: ::t: ::t: SAMPLES � � ��..:, � �;:: � � � � 111.111� � OU1� � � � �w rr, ::JS, .,.. ITI Q.-. N :::0 CD - BROTZEN C1) =.: Spiroplectammina laevis ::I: ::J en < incra ata REUSS Q) Neoflabellina ssleptodisca (ROEMER) 0 '-0 Cibicides beaumontianus � ::J (WEDEKIND) - Verneuilina limbata Q) ::::,- a- (d 'ORB.) -, 0 Orbignyna aragonitica 0 C1) - < - CUSHMAN "TI Q) ;a < - Osangularia lens HOFKER en Siphogaudryina ( Het.) fo veolata en < -- - BROTZEN a.: Eponides beisseli )> CD ( MARSSON) "7" s.en - Neoflabellina praereticulata(SCHIJFSMA) � --- Bolivinoides australis HILTERMAN Z :r- Neoflabellina reticulata : EDGELL ITI ::, Pseudoparrella alata "TI Bolivinoides draco draco(REUSS) =tJ C1) =· � (MARSSON) CD - > Allomorphina bullata ( MARSSON) () () cimbrica :::0 Q) ------_;• HOFKER l> m 3 (00 "O i------+------=------+-CD+ -- O ---.------ITI- ----....::._Reussella (TROELSEN) ""tl Q) ::J )> o, HOFKERGlobotruncana 's zones (1966) Globotruncana petaloidea iii"=;:i. I< .._ - gr. area (CUSHMAN) Rosita contusa :-T1 =· - cf. (GANO.) :-U I :, -- • --r.. (CUSHMAN) in B.& V. 1975 - - Reinhardtites anthophorus DEFLANDRE CD - () Broinsonia parca constricta HATTN. etal. :Il - m -- Amphizygus mini mus BUKRY z 0 - EiffeUi thus eximius (STOVER) )> iJ Phanutites obscurus ( DEFLAN ORE) z co - - Lucianorhabdus cay euxi DEFLANDRE z - - EiffeUithus turriseiffefi DEFL. & FERT. 0 -- "'tJ Prediscosphaera stoveri (PERCH. NIELSEN) I - r - Arkhangetskie((a cymbiformis VEKSHINA )> auadrum gothicum ( DEFL.) z Quadrum trifidum (STRADNER) ::,;: - - -I --;;,.. Reinhardtites levis PRINS . & SISSINGH. 0 Li thraphidites praequad r atus ROTH z () � Lithraphi di tes quadratus BR. & MART. l> � Brolnsonia parca constricta zone IPr.stoveri z. Lithraphidites praequadratus zone I Lithr. quadr. zone � - z DEFL. - Pataeohystrichophora infusorioides j;; z - Thafassiphora ? spinosa (CLARKE & VERD.) CJ Afdorfia deftandrei (CLARKE & VERD.) - z � Hystrichodinium putchrum DEFL. 0 i.-- CJ)� Odontochitina opercutata (0. WETZ.) -i - r,, :Il - Xenascus ceratioides ( DEFLANDRE) n - - Senoniasphaera reticutata in WILSON )> ::r: G) -i - Odontochitina wetzefi in WILSON j;; GiWnia hymenophora COOKS & EI SEN . rn z -- - r Areotigera senonensis LEJ.-CARP. CD r 0 - Samlandia sofida in WILSON )> C -I z -- -> Spongodinium defitiense (EHRENBERG) 0 in WILSON rn l> Northidinium perforatum Ul :Il ---- Tri btastuta utinensis 0. WETZEL -< z m -- Trudopo((is nonperfectus (PFLUG) PFLUG z l> -- FelderipoUenites triangutus KEDV. & HERN. 0 :Il /nterporopo((enites turgidus lSCH. + sp.1 :::0 � - Trudopo({ is artifex WEYL. & KRIEGER � CJ)� - Semiocufopoffis et. verrucosa CHRIST. )> -i :Il - Normapolle B � ::r:n - Vacuopoflis munitus TSCHUDY r -i - Pompeckjoidaepo((en. subhercynicus (KR.) KR . r - SantonipoUis sp. 1 rn - Extrapo Ws sp.1 AZEMA et al. Ul 0 o-', VI I ., i.,.. VI N ,o 3(..)1 0 3 0 1'11 n Ul 0� .r-- 0 a> zn 0 -I ;- DI I jU'3 0 ITI 0 3 / i:...... � � CJ) I UlCJ � -, - � I I N 1'11 N on 0�rn - w ffl- Ul CJ)�o I 0) (/lr-0 I 62 F. ROBASZYNSKI ET COLL. BCREDP 9 (1985)

Lithraphidites quadratus appears only at the top qf uppermost part represented by the Maastricht the Lixhe 3 Member. It seems that the entries of Formation). the Maastricht area was under the Lithraphidites praequadratus, Prediscosphaera influence of Boreal conditions with a relatively stoveri and Arkhange/skiella cymbiformis might deep sea. Only the Maastricht Formation was occur earlier in the Tethyan type-Campanian area deposited in shallow water under conditions than in the Boreal Maastrichtian area {cf. NEUMANN affected by some Tethyan influences. et al., 1984; NEUMANN & RoBASlYNSKI, 1985). The lateral and vertical variations of thicknesses in the diverse members such as the preservation • Dinoflagellates of sedimentary units in well delimited areas can be The species Samlandia so/ida appears in the interpreted as a recording of vertical movements Beutenaken Member whereas Areoligera seno of tectonic blocks whose existence is linked to the nensis comes a little before in the Upper Campa Rur Graben. nian Zeven Wegen Member.

• Spores and pollen grains 8. - REFERENCES The Zeven Wegen Member has not yielded material of terrestrial origin. The palynoflora in situ observed in the Vaals Formation. Beutenaken 1. Regional stratigraphy and historical review Member and Vijlen Member is not in a sufficient ALBERS. H.J. (1976). - Feinstratigraphie. Faziesana quantity and the assemblages are incomplete. lyse und Zyklen des Untercampans (Vaalser From a biostratigraphical point of view. some Grunsand = Hervian) von Aachen und dem obstacles preclude to correlate irrefutably the niederlandisch - belgischen Limburg. - Geol. Campanian-Maastrichtian boundary between Bo Jb .. A 34. 3-68. 17 fig.. 10 encl. real and Tethyan realms. These difficulties are of ALBERS. H.J .. FELDER. W.M.. FELDER, P.J. & KuvL. O.S. various nature. (1978). - Guide Book of the joint annual First. the palaeontological groups in the two meeting of the Palaontologische Gesellschaft and the Palaeontological Association. Maas realms are different: Belemnites are numerous tricht. 25.09-1.10.1978. Exe. A : Lithology and and vertically well distributed in the Boreal realm stratigraphy of Upper Cretaceous of Eastern and practically absent in the Tethyan realm. plank South-Limburg including adjacent Belgium tonic Foraminifera are very well diversified in German borderland. Exe. C : Lithology and pelagic Tethyan environment and very rare in the stratigraphy of Upper Cretaceous of the Bel Boreal realm. small benthic forms occur in the gium-Dutch borderland west of the River Boreal against large benthic forms in the Tethyan Meuse. - 100 p .. 56 fig. realm. ARKHANGELSKY. A.O. (1912). - Verchne melowye Furthermore. the entries of several species of vostoka Jevropejskoj Rossii. - Materialy dla Nannoplankton seem to be diachronous between geologii Rossii, 25. 631 p .. 18 tabl., 10 pl. (en the two realms. Besides. the data for the distribu russe). tion of Dinoflagellates in the Tethyan realm are not BERGGREN, W.A. (1964). - The Maastrichtian. sufficiently numerous to be compared to that of Danian and Montian Stages and the Creta the Boreal realm. ceous-Tertiary boundary. - Stockh. Contr. Geol., 11. 103-175. 5 tab I. From a palaeoecological point of view. the BINCKHORSTVAN DEN 81NCKHORST. J.J.-T. VAN (1859). - presence of numerous reworked Spores and Esquisse geologique et paleontologique des pollen grains from the Jurassic to the Lower couches cretacees du Limbourg et plus specia Cretaceous in the Vaals Formation points out the lement de la craie Tuffeau. - Ed. van Osch existence of rather important currents during the America & Cie. Maastricht. 268 p .. 5 pl.. 1 geol. deposition of this unit. Moreover. the characteris map. tics of the sea seem to be the same during the BINCKHORSTVAN DEN 81NCKHORST, J.J.-T. VAN (1860). - deposition of about the whole of the Gulpen Sur la craie de Maestricht et sur les fossiles de Formation. cette localite. - Bull. Soc. geol. France. (2). 17. 61-66. That suggests an open marine environment. relatively quiet and rather far from the shore. BINCKHORSTVAN DEN BINCKHORST. J.J.-T. VAN (1861). - Monographie des gasteropodes et des cepha That is to say that. during the Upper Campanian lopodes de la craie superieure du Limbourg. and a great part of the Maastrichtian (except the suivie d'une description de quelques crustaces BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 63

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Legende generale de la carte geologique detailJee PusN1ER-lADAME, F. & CouPATEZ. P. (1969). - Etude de la Belgique (1929). - Ann. Mines Belg., 30. morphologique de l'anneau sclerotique de 39-80. Mosasaurus hoffmanni MANTELL. 1829. - Bull. LERICHE. M. (1927). - Les Poissons du Cretace Soc. beige Geol.. Pa/eontol., Hydro/., 78, marin de la Belgique et du Limbourg hollan 253-265, 9 fig. dais. Note preliminaire. Les resultats stratigra ROBASZYNSKI, F .. BLESS, M.J.M.. FELDER, P.J., FOU phiques de leur etude. - Bull. Soc. beige CHER, J.C.. LEGOUX. 0., MANIVIT, H., MEES Geol., Paleontol., Hydro/., 37, 199-299. 1 tabl., SEN, J.P.M. Th. & VAN DER TuuK, L.A. (1985). - La 19 fig. limite Campanien-Maastrichtien dans le Lim MEIJER. A.W.F. (1984). - Tanden van Mosasaurus bourg belgo-neerlandais. - Geol. Medit., 10, lemonnieri DOLLO, 1889 (Reptilia, Mosasauri 3-4, p. 59-72, 6 fig. dae) in Limburgse Krijtafzettingen. - Natuur RoMEIN, B.J. (1962). - On the type locality of the hist. Maandbl., 73, 146-148, 1 fig. Maastrichtian (DUMONT. 1849), the upper boun NAIDIN, D.P. (1983). - The Upper Cretaceous dary of that stage and on the transgression of Stage boundaries of the East part of the Maastrichtian s.l. in Southern Limburg. - Me European palaeobiogeographic Reg.ion. - In: ded. geol. Sticht., N5, 15. 77-84, 5 fig. BIRKELUND, T. et al. {ed.) : Cretaceous Stage ROMEIN, B.J. (1963). - Present knowledge of the Boundary Symposium Abstracts, 140-142. stratigraphy of the Upper Cretaceous NEUMANN, M. (1980). - Campanien. In: CAVELIER, C. (Camp.-Maastr.) and Lower Tertiary (Danian & ROGER. J. {ed.) : Les etages francais et leurs Montian) calcareous sediments in Southern stratotypes. - Mem. Bur. Rech. geol. min., 109, Limburg. - Verh. K. nederl. geol. mijnbouwkd. 161-170. 3 fig., 4 tabl. Genoot., geol. Series, 21. 2, 93-104, 6 fig. NEUMANN, M., ANDREIEFF, P., LAMBERT, B. & PLA Rurnr, A. (1894). - Essai de synchronisme des TEL, J.P. (1984). - Un exemple precis du couches maastrichtiennes et senoniennes de passage Campanien-Maastrichtien en facies Belgique. du Limbourg hollandais et des envi neritique : la region de Maurens. Dordogne rons d'Aix-la-Chapelle. - Bull. Soc. beige (France). - C.R. Acad. Sci. (Paris) (2), 298. Geol., Paleontol., Hydro/., M145-194, 5 fig., 845-850. 1 pl.-tabl. 1 tabl. NEUMANN, M. & RosASZYNSKI. F. (1985). - Tentative RuTOT, A. & VAN DEN BROECK, E. (1887). - Observa de comparaison entre la limite superieure du tions nouvelles sur le Cretace superieur de la Campanien stratotypique et la limite inferieure Hesbaye et sur les facies peu connus qu'il du Maastrichtien stratotypique. - Geol. Medit., presente. - Bull. Soc. beige Geol., Paleontol., 10, 3-4. Hydro/., 1. M113-164. 11 fig .. 1 tabl. 0MALIUS d'HALLOY, J.J. d' (1808). - Essai sur la SCHMID. F. (1967). - Die Oberkreide-Stufen Cam geologie du Nord de la France. Journ. Mines. pan und Maastricht in Limburg (Sudnieder 24. p. 123-158. lande, Nordostbelgien). bei Aachen und in 0MALIUS d'HALLOY, J.J. d' (1828). - Memoires pour Nordwestdeutschland. - Ber. cJ.tsch. Ges. geol. servir a la description geologique des Pays-Bas. Wiss., 12. 471-478. 1 fig. de la France et de quelques contrees voisines. SCHULZ. M.-G. (1978). - Zur Litho- und Biostrati Imp. Gerard. Namur; 307 p., 1 pl. graphie des Obercampan-Untermaastricht von

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HoFKER. J. (1958 b). - Upper �retaceous Bolivinoi DOEVEN. P.A. (1983). - Cretaceous nannofossil des guide forms. - M,cropaleontology, 4. stratigraphy and paleoecology of the Canadian 329-333. 2 pl. Atlantic Margin. - Bull. geol. Surv. Canada, 3. HoFKER. J. (1961). - Foraminifera from the Creta 56. 1-70. 27 fig., 6 pl. ceous of South-Limburg. Netherlands. LII. HATINER, J.G .. WIND, F.H. & WISE, S.W. (1980). - Stratigraphy of the Gulpen Chalk in South The Santonian/Campanian boundary : compa Limburg established by means of _the Orthoge rison of nearshore-offshore calcareous nanno nesis of Bolivinoides. - Natuurh,st. Maandbl., fossils assemblages. - Cah. Micropaleont .. 3. 50. 37-40. 2 diagr. 9-26. HOFKER. J. (1961). - The foraminifera of t�e Upper· LAMBERT. B. (1980). - Etude de la Nannoflore Campanian-Maastrichtian boundary 1n South calcaire du Campanien charentais. - Cah. Limburg. Netherlands. - N�tuurhist. Ge Micropaleont., 3. 39-53. 6 fig .. 1 pl. nootsch. Limburg, 12. 46-54. 5 fig. MARTINI, E. (1976). - Cretaceous to recent calca HOFKER. J. (1966). - Maastrichtian. Danian �nd reous nannoplankton from the Central Pacific ocean (D.S.D.P .. Leg. 33). - Paleocene foraminifera. - Palaeontograph1ca. /nit. Rep. DSDP, 383-423. 13 pl. suppl. 10. 1-2). 376 p .. 178 fig .. 69 tabl.. 44 fold .. 33. 86 pl. PERCH-NIELSEN, K. (1972). - Remarks on Late Cretaceous to Pleistocene coccoliths from the K1MPE. W.F.M.. BLESS. M.J.M. et al. (1978). - North Atlantic. - /nit. Rep. DSDP, 14. Paleozoic deposits east of the Brabant Massif in 1003-1069. 1 text-fig .. 7 tabl.. pl. 1-22. Belgium and the Netherlands. - Meded. Rijks Geol. Dienst., 30. 37-102. 12 fig .. 5 tabl.. 16 pl.. PERCH-NIELSEN, K. (1977). - Albian to Pleistocene 7 encl. calcareous nannofossils from the Western South Atlantic. - /nit. Rep. DSDP, 39, 699-823. MEESSEN. J.P.M.Th .. SCHUMACKER-l.AMBRY, J. & VAN 50 pl.. 23 tabl. GUESTAINE M. (1978). - Biostratigraphy of the PERCH-NIELSEN. K. (1979). - Calcareous nannofos Upper Cretaceous in South Limburg. - In: Introduction to the excursions of the Palaont. sils from the Cretaceous between the North Sea Gesellsch. - Palaeontol. Ass .. Maastricht, 25-9 and the Mediterranean. - Aspekte der to 1-10-1978. 10-15. 1 fig. Kreide Europas. IUGS. A 6. 223-272. PERCH-NIELSEN. K. (1983). - Recognition of Creta RoBASZVNSKI. F.. CARON. M .. GONZALEZ DoNoso. J.M. ceous stage boundaries by means of calca & WONDERS. A.A.H. (editors and European reous nannofossils. - In : B1RKELUND. T. et al. : Working-Group on Planktonic Foraminifera) Abstracts of the Symposium on Cretaceous (1984). - Atlas of_ Late �retaceous Globotrun Stage Boundaries. 152-156. 1 tabl. canids. - Rev. M,cropaleont., 26. 3-4. 145-305, 11 text-fig.. 54 pl. ROTH. P. (1978). - Cretaceous nannoplankton biostratigraphy and oceanography of the SCHIJFSMA. E. (1946). - The Foraminife�a from the Northwestern Atlantic ocean. - /nit. Rep. Hervian (Campanian) of Southern Limburg .. - DSDP, 44. 731-759. 11 fig., 3 pl., 1 tabl. ser. C.V.. 174 p.. 5 fig .. Meded. geol. Sticht.. 7. S1ss1NGH. W. (1977). - Biostratigraphy of Creta 4 tabl.. 10 pl. ceous calcareous nannoplankton. - Geol. en VAN R1Js1NGE. C.P.J. (1932). - Description of some Mijnb., 56, 1, 37-65. Foraminifera of a boring near Bunde (Dutch South Limburg). - Thesis. Amsterdam; 112 p. THIERSTEIN, H.R. (1976). - Mesozoic calcareous nannoplankton biostratigraphy of marine sedi VILLAIN. J.M. (1977). - Le Maastrichti�n dans sa_ ments. - Marine Micropa/eont., 1, 325-362. region type (Limb_ourg. ays-Bas . Etude strat1- � � WANGEROW. E.F. & SCHLOEMER, W. (1967). - Ver graphique et m1cropaleontolog1que .. - Pa A 157. 1-87. 28 text-fig .. 13 pl. gleich des « Vetschauerkalkes » des Aachener_ laeontographica. Kreide mit dem Kreide-Profil von Sud-Limburg anhand von Coccolithen. - Geol. en Mijnb., 46. 453-458. 8 fig. 4. Nannoplankton VERBEEK. J.W. (1977). - Calcareous nannoplankton biostratigraphy of Middle and Upper Creta CEPEK. P. & HAY. W.W. (1969). - Calcareous ceous deposits in Tunisia. Southern Spain and nannoplankton and biostratigraphic subdivision France. - Utrecht Micropaleont. Bull., 16. of the Upper Cretaceous. - Trans. Gulf Coast. 1-157. 12 pl., 21 fig. 19. 323-336 Assoc. Geol. Soc., VERBEEK. J.W. (1983). - The calcareous nannofos CRux. J.A. (1982). - Upper Cretaceous (Cenoma_ sils from the Campanian and Maastrichtian nian to Campanian) calcareous nannofossils. - rocks of Southern Limburg (the Netherlands) In: LORD. A.R. (ed.). : A Stratigraphical Index of and the adjacent Belgian area. - In: B1RKELUND. Calcareous Nannofossils. 81-135. 10 pl.. 3 tabl.. T. et al. : Abstracts of the Symposium on 5 fig.. Horwood. Chichester. ' Cretaceous Stage Boundaries. 197-200. 1 fig. F. ROBASlYNSKI ET COLL. BCREDP 9 (1985) 68

5. Dinoflagellates • 6. Spores and pollen grains CONRAD, W. (1941 ). - Notes protistologiques. XIX. AzEMA, C., FAUCONNIER, D. & VIAUD, J.M. (1981). - Ouelques microfossiles des silex cretaces. - Microfossils from the Upper Cretaceous of Bull. Mus. roy. Hist. nat. Belg., 17, 36. 1-10. Vendee (France). - Rev. Palaeobot. Palynol., 3 fig., 1 pl. 35, 237-281. FoucHER, J.-C. (1979). - Distribution stratigraphi CouPER, R.A. (1958). - British mesozorc microspo que des kystes de Dinoflagelles et des Acritar res and pollen grains. A Systematic and Strati ches dans le Cretace superieur du Bassin de graphic Study. - Palaeontographica, B. 103, Paris et de !'Europe septentrionale. - Palaeon 75-179, pl. 15-31. 11 fig., 12 tabl. tographica. B. 169, 1-3, 78-105, 1 fig., 4 tabl. DbRHbFER, G. (1977). - Palynologie und Stratigra FOUCHER, J.-C. & ROBASZYNSKI, F. (1977). - Micro phie der Buckeberg - Formation (Berriasium - plancton des silex du Bassin de Mons (Belgi Valanginium) in der Hilsmude (NW - Deuts que) (Dinoflagelles cretaces et daniens). - chland). - Geol. Jb., (A.). 42, 3-122. 15 pl., Ann. Paleont. {lnvertebres), 63. 1. 19-58. 3 fig., 8 fig., 3 tabl. 2 tabl., 7 pl. DbRHOFER, G. (1979). - Distribution and stratigra LEJEUNE, M. (1937). - L'etude microscopique des phic utility of Oxfordian to Valanginian miospo silex. Un fossile anciennement connu et pour res in Europe and North America. - AASP tant meconnu : Hystrichosphaera ramosa Contributions (5 B), 2, 101-132, 3 pl. Ehrbg. (Deuxieme Note). - Ann. Soc. geol. KrnvEs. M. & HERNGREEN. G.F.W. (1980). - Palyno Belg., 60, B239-260. 2 pl. logy of the stratotype of the Maestrichtian and LEJEUNE-CARPENTIER, M. (1951). - L'etude micros the Gulpen formation. ENCi Section, Maas copique des silex. Gymnodinium et Phanerodi tricht the Netherlands. - Pollen et Spores, 22. nium (Dinoflagellates) de Belgique (Treizieme 3-4, 483-544. Note). - Ann. Soc. geol. Belg., 74. B3G7-3i3. NORRIS. G. (1969). - M1ospores from the t'urbeck 8 fig. Beds and marine Upper Jurassic of southern LENTIN, J.K. & WILLIAMS, G.L. (1981 ). - Fossil England. - Palaeontology, 12. 4, 574-620, Dinoflagellates : index to genera and species. pl. 102-113 1981 edition. - Report series. Bedford Institute SINGH, C. (1971). - Lower Cretaceous Microfloras of Oceanography, BI-R-81-12. VII + 345 p. of the Peace River Area, Northwestern Alberta. ScHUMACKER-lAMBRY, J. (1977). - Microfossiles - Bull. Res. Counc. Alberta, 28. 2 vol. + App. : vegetaux? planctoniques. - In: STREEL M. 1-542, 80 pl., 75 fig.; Edmonton. et al. : Macro- et biostratigraphique du Seno VANGUESTAINE, M. & STREEL, M. (1977). - Spores nien-Paleocene de la rive gauche de la Meuse and pollens. - In: STREEL M. et al. : Macro- et au nord de Liege, Belgique. Livret-gui9e de microfossiles vegetaux dans le contexte litho-et !'excursion du 22 septembre 1977, a !'occasion biostratigraphique du Senonien-Paleocene de du symposium « Apport des techniques recen la rive gauche de la Meuse au Nord de Liege. tes en Palynologie », 45-53, 2 fig., 7 pl.; INIEX Belgique. Livret-guide exc. symp. « Apport des Univ. Liege. techniques recentes en palynologie ». 71-73. INIEX - Univ. Liege. STOVER, L.E. & Ev1n, W.R. (1978). - Analyses of pre-Pleistocene organic-walled Dinoflagellates. TscHUDY, R.H. (1975). - Normapolles Pollen from - Stanford Univ. Pub/.. geol. Sci .. 15. 300 p., the Mississippi Embayment. - U.S. Geol. Surv. 2 fig., 6 tabl. Prof Paper, 865. 1-42. VANGUESTAINE. M. (1966). - Etude palynologique WILSON, G.J. (1971). - Observations on European quantitative dans deux carrieres du Cretace late Cretaceous dinoflagellate cysts. - In : superieur de la vallee de la Meuse. - Bull. Cl. FARINACCI, A. (ed.) : Proceedings of the 2nd Sci. Acad. roy. Belg., 5, 52, 1534-1548, 11 fig. Planktonic Conference (Roma 1970), 1259-1275. 1 fig., 4 pl. Tecnoscienza. Roma. 7. Ostracods and mesofossils WILSON, G.J. (1974). - Upper Campanian and Maastrichtian dinoflagellate cysts from the BLESS, M.J.M. (1983). - Late Devonian and Carbo Maastricht region and Denmark. - Ph. D. Univ. niferous ostracode assemblages and their rela Nottingham, V + 601 p., 59 fig., 3 tabl., 35 pl. tionship to the depositional environment. - Bull. Soc. beige Geol., 92, 31-53. W1T. R. de (1943). - Hystrichosphaeridae uit BLESS, M.J.M. et al. (1983). - Ostracoden uit het Limburgsche vuursteen. - Verh. K. nederl. Boven-Krijt van Zuid-Limburg als milieu-indika 13, 363-392. 15 fig., 2 tabl. geol.-mijnb. Gen., toren. - Natuurhist. Maandbl., 158-164, 4 fig. W1T, R. de (1944). - Micro-organismen in Lim BosouET, J. (1847). - Description des Entomostra burgsche vuursteen. - Natuurhist. Maandbl., ces fossiles de la craie de Maestricht. - Mem. 7-8, 52-55, 6 fig. Soc. roy. Sci. Liege, 4, 353-378. 4 pi. BCREDP 9 (1985) CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT 69

BosauET. J. (1854). - Monographie des crustaces ROgen. - Palaont. Abh.. A. 2. 693-1024. fossiles du terrain cretace du duche du Lim 114 Abb .. 45 Taf. bourg. - Verh. Geol. Beschnjving Kaart Ned., KozuR, H. (1972). - Die Bedeutung triassicher 2, 52-126. 7 pl. (Kruseman. Haarlem). Ostracoden fur stratigraphische und palaooko CLARKE. B. (1982). - Die Gattung Cytherelloidea logische Untersuchungen. - Mitt. Ges. Geol. ALEXANDER. 1929 (Ostracoda) im Schreib Bergbaustud.. 21. 661-710. kreide-Richtprofil von Lagersdorf-Kronsmoor L1EBAu. A. (1976). - Entwurf einer palaobathyme Hemmoor (NW-Deutschland). - Geo/. Jb., trischen Flachmeer-Zonierung mit Hilfe von A61. 35-71. Ostracoden und anderen Mikrofossilien. - Zbl. CLARKE. B. (1983). - Die Cytheracea (Ostracoda) Geol. Palaont.. (2) 1976. 442-447. im Schreibkreide-Richtprofil von Lagerdorf ROBASZYNSKI, F.. BLESS, M.J.M .. FELDER. P.J.. FOU Kronsmoor-Hemmoor (Coniac bis Maastricht; CHER, J.C.. LEGOUX, 0.. MANIVIT, H.. MEES Norddeutschland). - Mitt. Geol. Palaont. Inst. SEN. J.P.M. Th. & VAN DER TuuK, LA (1985). -'- La Univ. Hamburg, 54. 65-168. 15 pl., 17 fig.. 3 tabl. limite Campanien-Maastrichtien dans le Lim DERoo. G. (1966). - Cytheracea (Ostracodes) du bourg belgo-neerlandais. - Geol. Medit., 10. Maastrichtien de Maastricht (Pays-Bas) et des 3-4. p. 59-72. 6 fig. regions voisines; resultats stratigraphiques et ROMEIN, 8.J., SCHUURMAN, H. & LISSENBERG. Th. paleontologiques de leur etude. - Meded. ° (1977). - De foraminiferen en ostracoden van Geol. Sticht., Ser. C. 46. 2. n 2. 1-187. 22 fig.. de Kunrader Kalk van weginsnijding 628293 bij 27 pl.. 9 tabl. Benzenrade. - Grondboor en Hamer. 31 (6) : FELDER, P.J. (1981 ). - Mesofossielen in de kalkaf 173-181. zettingen uit het Krijt van Limburg. - Pub/. Nat. VAN VEEN. J.E. (1932). - Die Cytherellidae der Hist. Genootsch. Limburg, 31. 1-2. 1-35. Maastrichter Tuffkreide und des Kunrader Kor FELDER. P.J. (1982). - Mesofossils in the Creta rallenkalkes von Sud-Limburg. - Verh. Geol. ceous chalk of Heugem-1 and Kastanjelaan-2. Mijnb. Genoots. Nederland. Kol. Geol. ser. 9. - Pub/. Nat. Hist. Genootschap Limburg, 32, 317-364. 1-4. VAN VEEN. J.E. (1934-1937). - (reeks va� tweeent FELDER. W.M. (1977). - De stratigrafische plaats wintig artikelen over ostracoden u1t het B_o van de« Kunrader Kalksteen » in het Boven-Krijt ven-Krijt van Zuid-Limburg). - Natuurh,st. Maandbl.. 23 : 88-95. 103-11. 115-122. 128-132; van Zuid-Limburg. - Grondboor en Hamer, 6, 24 : 26-28. 32-36, 48-51. 56-60. 83-88, 95-98. 163-172. 106-112; 25 : 21-24. 32-36. 42-45. 61-64. 69-71. HERRIG, E. (1966). - Ostracoden aus der Weissen 82-86. 98-101. 108-113, 131-188; 27: 10-12, Schreibkreide (Unter Maastricht) der lnsel 15-20.

LIST OF PLATES

1-2-3 Belemnites 4-5-6 Benthic Foraminifera 7-8 Nannoplankton 9-10-11-12 Dinoflagellates 13-14 Normapolles 15 Reworked Spores and pollen grains 16-17-18 Mesofossils 19-20-21-22 : Ostracods • BCREDP 9 (1985) 70 F ROBASZYNSKI ET COLL.

PLATE 1 BELEMNITES

Fig. 1 - Gonioteuthis quadrata (BLAINVILLE. 1827) Length = 67 mm Vaals Formation, C.P.L. Halembaye Collection Teylers Museum. Haarlem. no. 25053 a. ventral view. b. lateral view 2. - Belemnitella mucronata (LINK. 1807) Length = 98 mm Zeven Wegen Member. lower part. C.P.L. Halembaye Collection W.M. FELDER, Vijlen, no. GK1914 a. ventral view. b. lateral view 3. - Belemnitella mucronata (LINK. 1807) Length = 104 mm Zeven Wegen Member, upper part. Malensbosch Collection W.M. FELDER, Vijlen. no. GK1485A3 a. ventral view. b. lateral view BCREDP 9 (1985) F. ROBASlYNSКI ЕТ COLL. CAMPANIAN-MAASTRICHTIAN 71 BOUNDARY NEAR MAASTRICHT Plate 1 72 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 2 BELEMNITES

Fig. 1 - Belemnitella mucronata "minor" sensu JELETZKY, 1949 Length = 88 mm Zeven Wegen Member, upper part, C.P.L. Halembaye Collection Teylers Museum, Haarlem, no. 25057 a. ventral view, b. lateral view

2. - Belemnitella mucronata "minor" sensu JELETZKY, 1949 Length = 84 mm Zeven Wegen Member, upper part, Plattebosch Collection W.M. FELDER, Vijlen, no. GK1267 a. ventral view, b. lateral view

3. - Belemnitella lanceolata inflata (ARKHANGELSKY, 1912) Length = 72 mm Beutenaken Member, upper part, Bovenste Bosch, Epen Collection Teylers Museum, Haarlem, no. 25058 a. ventral view, b. lateral view BCREDP 9 (1985) ROBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN 73 BOUNDARY NEAR MAASTRICHT Plate 2 74 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 3 BELEMNITES

Fig. 1 - Belemnella « occidentalis » sensu B1RKELUND, 1957 Length = 94 mm Beutenaken Member, upper part Bovenste Bosch, Epen Collection Teylers Museum, Haarlem, no. 25063 a. ventral view. b. lateral view

2. - Belemnitella junior NOWAK, 1913 Length = 90 mm Lixhe Member, C.P.L. Halembaye Collection Teylers Museum, Haarlem, no. 25067 a. ventral view, b. lateral view

3. - Belemnite/la junior NowAK, 1913 Length = 103 mm Vijlen Member. lower part Kosberg, Epen Collection W.M. FELDER, Vijlen. no. GK2020 a. ventral view, b. lateral view 3CREDP 9 (1985) ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 75 BOUNDARY NEAR MAASTRICHT Plate 3 76 F ROBASZVNSKI ET COLL. BCREDP 9 (1985)

PLATE 4 BENTHIC FORAMINIFERA

The bar on each photograph represents 100 micrometres; a = spiral side; b = umbilical side

Fig. 1. Gavelinella clementiana (o·ORBIGNY) Sample H 82-1

2. Gavelinella clementiana (o·ORBIGNY) Sample H 82-5

3. Stensioeina pommerana (BROTZEN) Sample H 82-8

4. - Pseudoparrella alata (MARssoN) sensu HoFKER. 1966 Sample H 82-12 BCREDP 9 (1985) ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 77 BOUNDARY NEAR MAASTRICHT Plate 4 78 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 5 BENTHIC FORAMINIFERA

The bar on each photograph represents 100 micrometres; a = spiral side; b = umbilical side

Fig. 1. Neoflabellina leptodisca (WEDEKIND) Sample H 82-7

2. Neoflabellina praereticu/ata HILTERMANN Sample H 82-3

3. Neof/abellina reticulata (REuss) Sample H 82-11

4. Bolivinoides draco (MARSSON) Sample H 82-15

5. Gavelinopsis monterelensis (MARIE) Sample H 82-6

6. Eponides beisse/i ScHIJFSMA Sample B 82-2

7 - Bolivina incrassata REuss Sample H 82-10 :CREDP 9 (1985) ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 79 BOUNDARY NEAR MAASTRICHT Plate 5 F ROBASlYNSKI ET COLL. BCREDP 9 (1985) 80

PLATE 6 BENTHIC FORAMINIFERA THE BOLIVINOIDES DECORATA-AUSTRALIS LINEAGE

The bar on each photograph represents 100 micrometres

Fig·. 1. Bolivinoides decorata (JONES) Sample H 82-3. with 3 pustules on the last formed chamber

2. Bolivinoides decorata (JONES) Sample H 82-4. with 4 pustules on the last formed chamber

3. Bolivinoides australis EDGELL Sample H 82-2, with 5 pustules on the last formed chamber

4. Bolivinoides australis EDGELL Sample H 82-11, with 5 pustules on the last formed chamber

5. Bolivinoides australis EDGELL Sample H 82-11. with 6 pustules on the last formed chamber

6. - Bolivinoides australis EDGELL Sample H 82-11, with 7 pustules on the last formed chamber BCREDP 9 (1985) ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 81 BOUNDARY NEAR MAASTRICHT Plate 6 82 F ROBASZYNSKI ET COLL. BCREDP 9 (1985)

PLATE 7 NANNOPLANKTON

The bar on each figure represents 1 micrometre

Fig. 1 Broinsonia parca (STRADNER) Distal view

2. Eiffellithus eximius (STOVER) Distal view

3. Broinsonia enormis (SHUMENKO) Proximal view

4. Ahmuellerella regularis (GORKA) Distal view

5. Ahmue/lerella octoradiata (GORKA) Distal view

6. Kamptnerius magnificus DEFLANDRE Distal view

7 Reinhardtites anthophorus DEFLANDRE Side view

8. Gartnerago obliquum (STRADNER) Distal view

9 Tranolithus orionatus STOVER Side view

10. Prediscosphaera stoveri (PERCH-NIELSEN} Distal view

11 Lucianorhabdus cayeuxi DEFLANDRE

12. Amphizygus brooksi BuKRY Distal view BCREDP 9 (1985) F ROBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN 83 BOUNDARY NEAR MAASTRICHT Plate 7 84 F ROBASZYNSKI ET COLL BCREDP 9 (1985)

PLATE 8 NANNOPLANKTON

The bar on each figure represents 1 micrometre

Fig. 1 Ouadrum gothicum (STRADNER)

2. Microrhabdulus decoratus DEFLANDRE

3. Micula staurophora (GARDET) Proximal view

4. Reinhardtites anthophorus DEFLANDRE Proximal view

5. Arkhangelskiella cymbiformis VEKSHINA Proximal view

6. Amphizygus broosksi BuKRY Distal view

7 Prediscosphaera cretacea (ARKHANGELSKY) Distal view 8. Markalius circumradiatus (Srnvrn) Proximal view

9. Reinhardtites /evis PRINS & S1ss1NGH Distal view

10. Lithraphidites et. praequadratus RoTH Proximal view

11 Lithraphidites et. praequadratus RoTH Distal view

12. - Lithraphidites quadratus BRAMLETIE & MARTINI Side view BCAEDP 9 (1985) F AOBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN 85 BOUNDARY NEAR MAASTRICHT Plate 8 86 F. ROBASZVNSKI ET COLL. BCREDP 9 (1985)

PLATE 9 DINOFLAGELLATES

The bar on each figure represents 10 micrometres

Fig. 1. - Kleithriasphaeridium et. truncatum (BENSON) STOVER & EvlTT Lixhe Member. Upper Maastrichtian Sample HAL. 82-11. Preparation 54732-1. N31. Precingular archeopyle·

2. - Kleithriasphaeridium cf. truncatum (BENSON) STOVER & Ev1n Vijlen Member. Upper Maastrichtian Sample HAL. 82-9. Preparation 54730-1. G46.1

3. - Laticavodinium gracilispinosum in WILSON and Fromea sp. Zeven Wegen Member. Upper Campanian Sample HAL. 82-6. Preparation 54715-1. F38.4

4. - Heterosphaeridium? heretacanthum (DEFLANDRE & COOKSON) EISENACK & l<.JELLSTROM Vaals Formation. Lower Campanian Sample HAL. 82-1. Preparation 54710-1. V28.1 Apical archeopyle

5. - Hystrichodinium pulchrum DEFLANDRE Zeven Wegen Member. Upper Campanian Sample HAL. 82-3. Preparation 54712-1. K39.1

6. - Cyclonephe/ium distinctum DEFLANDRE & COOKSON Vaals Formation. Lower Campanian Sample HAL. 82-1. Preparation 54710-1. G23.3. Apical archeopyle

7 - Pterodinium cingulatum cingulatum ( 0. WETZEL) BELOW Vaals Formation. Lower Campanian Sample HAL. 82-1. Preparation 54710-1. L28.2. Precingular archeopyle

8. 9. - Thalassiphora? Spinosa (CLARKE & VERDIER) FOUCHER Vaals Formation, Lower Campanian Sample HAL. 82-1. Preparation 54710-1, U48.1

10. 11. - Senoniasphaera reticulata in WILSON Vaals Formation. Lower Campanian Sample HAL. 82-2, Preparation 54711-1, J45. Apical archeopyle

12. - Gillinia hymenophora COOKSON & EISENACK Zeven Wegen Member. Upper Campanian Sample HAL. 82-5. Preparation 54714-1, K21.3

• The following data have been added for each specimen (1) The number of the sample HAL. 82-11. (2) The number of the preparation 54732-1 (slides are deposited at the Laboratoire de Palyno-Planctologie de la Societe Nationale Elf Aquitaine, in Boussens. 31360 Saint-Martory). (3) Co-ordinates with England Finder N31. BCAEDP 9 (1985) F ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 87 BOUNDARY NEAR MAASTRICHT Plate 9

. . .r' . 1--.· ,·. · • •• �-� . ... ·l

1 ..:...._ . 2 3

4 6

7 9_

11· 10 12 88 F ROBASZVNSKI ET COLL. BCREDP 9 (1985)

PLATE 10 DINOFLAGELLATES

The bar on each photograph represents 10 micrometres

Fig. 1 - Odontochitina costata ALBERTI emend. CLARKE & VERDIER Zeven Wegen Member. Upper Campanian Sample HAL. 82-6, Preparation 54715-1, E19. Apical archeopyle 2. - Odontochitina costata ALBERTI emend. CLARKE & VERDIER Zeven Wegen Member. Upper Campanian Sample HAL. 82-3, Preparation 54712-1, M28.4. Apical archeopyle 3. - Odontochitina costata ALBERTI emend. CLARKE & VERDIER Zeven Wegen Member. Upper Campanian Sample HAL. 82-3, Preparation 54712-1, N41.4. Operculum 4. - Xenascus ceratioides (DEFLANDRE) LENTIN & WILLIAMS Zeven Wegen Member. Upper Campanian Sample HAL. 82-6. Preparation 54715-1. U27.4. Apical archeopyle 5. - Xenascus ceratioides (DEFLANDRE) LENTIN & WILLIAMS Zeven Wegen Member. Upper Campanian Sample HAL. 82-6. Preparation 54715-1. H31 Apical archeopyle 6. - Xenascus ceratioides (DEFLANDRE) LENTIN & WILLIAMS Zeven Wegen Member. Upper Campanian Sample HAL. 82-6. Preparation 54715-1, U26.4. Operculum 7-8. - Odontochitina operculata (0. WETZEL) DEFLANDRE in DEFLANDRE & COOKSON Beutenaken Member, Lower Maastrichtian Sample BEUT 82-2, Preparation 55162-1, J34. A. specimen showing traces of a tabulation, paracingulum and apical archeopyle 9-10. - Odontochitina wetzeli in WILSON Zeven Wegen Member. Upper Campanian Sample HAL. 82-4, Preparation 54713-1, M36.1 Apical archeopyle 11-12. - Odontochitina wetze/i in WILSON Zeven Wegen Member, Upper Campanian Sample HAL. 82-7. Preparation 54716, 041.2. Apical archeopyle BCREDP 9 (1985) F ROBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT Plate 10 89 •·

� • • ..

1 ...- ,,_ - 2 3 - • y

\ ··"*II •. . ' • " .... 4 ··'·�, - _' .... .,.

.. 4- -• # • ,t. ,··.... •• . '! ••• . �:..}!· . // .,,... 9 • ·t 11

10 • - 12 90 F ROBASZYNSKI ET COLL. BCREDP 9 (1985)

PLATE 11 DINOFLAGELLATES

The bar on each photograph represents 10 micrometres

Fig. 1 - Areoligera senonensis LEJEUNE-CARPENTIER Vijlen Member. Upper Maastricht.ian Sample HAL. 82-9. Preparation 54730-1. E43.4. Apical archeopyle

2. - Areoligera senonensis LEJEUNE-CARPENTIER Vijlen Member. Upper Maastrichtian Sample HAL. 82-9. Preparation 54730-1. 047.3. Apical archeopyle

3. - Areoligera senonensis LEJEUNE-CARPENTIER Vijlen Member. Upper Maastrichtian Sample HAL. 82-9. Preparation 54730-1. F45.4. Apical archeopyle

4. - Areo/igera senonensis LEJEUNE-CARPENTIER Vijlen Member. Upper Maastrichtian Sample HAL. 82-1O. Preparation 54731-1. M27 1 Apical archeopyle

5. - Areo/igera cf. senonensis LEJEUNE-CARPENTIER Lixhe Member. Upper Maastrichtian Sample HAL. 82-12, Preparation 54733-1, J27 1 Operculum

6-7 - Areoligera coronata (0. WETZEL) LEJEUNE-CARPENTIER Lixhe Member, Upper Maastrichtian Sample HAL. 82-12. Preparation 54733-1. E27 1 Apical archeopyle

8. - Areoligera coronata (0. WETZEL) LEJEUNE-CARPENTIER ( = f. medusettiformis 0. WETZEL) Vijlen Member. Upper Maastrichtian Sample HAL. 82-9. Preparation 54730-1. 043.2. Apical archeopyle

9. - Areo/igera coronata (0. WETZEL) LEJEUNE-CARPENTIER ( = f. medusettiformis 0. WETZEL) Vijlen Member, Upper Maastrichtian Sample HAL. 82-9, Preparation 54730-1, U39.4. Apical archeopyle

10. - Areoligera coronata (0. WETZEL) LEJEUNE-CARPENTIER ( = f. medusettiformis 0. WETZEL) Vijlen Member, Upper Maastrichtian Sample HAL. 82-9, Preparation 54730-1. P40. Apical archeopyle

11 - Areoligera tenuicapi/lata (0. WETZEL) LEJEUNE-CARPENTIER Vijlen Member, Upper Maastrichtian Sample HAL. 82-9, Preparation 54730-1. 020.4. Apical archeopyle

12. - Areoligera tenuicapillata (0. WETZEL) LEJEUNE-CARPENTIER Vijlen Member. Upper Maastrichtian Sample HAL. 82-10, Preparation 54731-1. F32.3. Apical archeopyle BCREDP 9 (1985) F ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 91 BOUNDARY NEAR MAASTRICHT Plate 11

5 ......

12 92 F ROBASZVNSKI ET COLL BCREDP 9 (1985)

PLATE 12 DINOFLAGELLATES

The bar on each photograph represents 10 micrometres

Fig. 1-2. - Aldorfia deflandrei (CLARKE & VERDIER) STOVER & Ev1n Vaals Formation. Lower Campanian Sample HAL. 82-1. Preparation 54710-1. 020

3. - Spinidinium angustispinum in WILSON Vaals Formation, Lower Campanian Sample HAL. 82-2. Preparation 54711-1. L23.3

4. - Spinidinium angustispinum in WILSON Vaals Formation. Lower Campanian Sample HAL. 82-2. Preparation 54711-1. G35

5. - Northidinium perforatum in WILSON Vijlen Member. Upper Maastrichtian Sample HAL. 82-8, Preparation 54717-1. S34.4

6. - Northidinium perforatum in WILSON Vijlen Member. Upper Maastrichtian Sample HAL. 82-8. Preparation 54717-1. S43.1 Apical archeopyle and operculum

7 - Chytroeisphaeridia everricu/a in WILSON Vijlen Member. Upper Maastrichtian Sample HAL. 82-10. Preparation 54731-1. 036.3. Apical archeopyle

8. - Chytroeisphaeridia everricula in WILSON Zeven Wegen Member. Upper Campanian Sample HAL. 82-4. Preparation 54713-1. F29.3. Apical archeopyle

9-10. - Chytroeisphaeridia solida in W1LSON Zeven Wegen Member. Upper Campanian Sample HAL. 82-4. Preparation 54713-1. T23. Apical archeopyle

11-12. - Cladopyxidium sp. Zeven Wegen Member. Upper Campanian Sample HAL. 82-7. Preparation 54716. M15. Apical archeopyle

13. - Dinogymnium euc/aense COOKSON & EISENACK Zeven Wegen Member. Upper Campanian Sample HAL. 82-3. Preparation 54712-1. S29.3

14. - Gillinia hymenophora COOKSON & EISENACK Zeven Wegen Member. Upper Campanian Sample HAL. 82-3. Preparation 54712-1. F27.2 BCREDP 9 (1985) F ROBASZVNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT Plate 12 93

• • " • ,, • ., • 3 5 - . •

. ,

, . Ill . ,.".. ""

·,�>.. . " • .. . • ' .. 4 6 - •

f -;

JI> .

14 94 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 13 NORMAPOLLES All figures x 1CXJO

Fig. 1 a. b. Trudopollis non perfectus (PFLUG) PFLUG. 1953 2. Trudopollis sp. 1

3. Trudopol/is sp. 2

4. Trudopol/is sp. 2 5. ? Trudopollis sp. 4 6. lnterporopollenites turgidus TscHUDY. 1975

7 Semiocu/opol/is cf. sp. A TscHuov. 1975

8. Semioculopollis cf. verrucosa CHRISTOPHER. 1979

9. lnterporopollenites sp. 1

10. Trudopollis artifex WEYLAND & KRIEGER 1953

11 ?Hofkeripollenites sp.

12. Felderipollenites triangulus KEDVES & HERNGREEN. 1980

13. Extrapollis sp. 1 AzEMA et al.. 1981 14. Vacuopollis munitus TscHuov. 1975

15. Santonipollis sp. 1 BCREDP 9 (1985) F. ROBASZYNSKI ET COLL CAMPANIAN-MMSTRICHTIAN 95 BOUNDARY NEAR MMSTRICHT Plate 13

1a 2

3 4 5 l 6

' ,.·. ' =-. )I :

- . ·- .cJ �.�· ",..�·· ... -.=; -�--·· -., ..-.:-

7 8

10 12

•

14 15 96 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 14 NORMAPOLLES All figures x 1OOO

Fig. 1 a. b. - 2. Normapolle B 3 a. b. Extratriporopollenites sp. 1 4. Normapolle A. 5. Pseudotrudopollis pseudoalnus (KRuizscH) KRuizscH. 1967 6. ? Trudopollis sp. 3 7 Kriegeripollenites retigressus (WEYLAND & KRIEGER) KEDVES & HERNGREEN, 1980 8. Pompeckjoidaepollenites subhercynicus (KRuizscH) KRuizscH, 1967 9. Pompeckjoidaepollenites sp. 1 10. Normapolle C. 11. Normapolle D.

12-13. Amorphous organic matter with coccolith inclusions BCREDP 9 (1985) F ROBASZYNSKI ET COLL CAMPANIAN-MAASTRICHTIAN 97 BOUNDARY NEAR MAASTRICHT Plate 14 .,

1a 1b 2

3a 3b 4

11 F ROBASlYNSKI ET COLL. BCREDP 9 (1985) 98

PLATE 15 REWORKED SPORES AND POLLEN GRAINS All figures x 500

Fig. 1 lmpardecispora apiverrucata (COUPER) VENKATACHALA et al., 1968

2. Pilosisporites trichopapi//osus (THIEGART) DELCOURT & SPRUMONT, 1955

3. Concavissimisporites verrucosus DELCOURT & SPRUMONT, 1955

4. Neoraistrickia gristhorpensis ( COUPER) TRALAU, 1968

5. Sestrosporites pseudoalveolatus (CouPER) DETIMANN, 1963

6. Gleicheniidites triplex ( BOLCHOVITINA) DORING, 1965

7 Cerebropollenites mesozoicus (COUPER) NILSSON, 1958

8. Applanopsis trilobatus DORING, 1961

9. Laricoidites triquetru_s LANTZ, 1958

10. Corollina meyeriana (KLAus) VENKATACHALA & GocZAN, 1964

11-12. Corollina torosa (RE1ss1NGER) CORNET & TRAVERSE, 1975; fig. 11 well preserved specimens; fig. 12 slightly altered specimens BCREDP 9 (1985) F ROBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN BOUNDARY NEAR MAASTRICHT Plate 15 99

2 ..

8. 7

,.. .

10 11 12 100 F. ROBASZYNSKI ET COLL. BCREDP 9 (1985)

PLATE 16 MESOFOSSILS

Characteristic mesofossils from the ecozone 3, ENCi quarry, Maastricht

Fig. 1. Group Porifera. Bryozoa. Octocorallia. Grafularia 2. Group Mollusca. Brachiopoda 3. Group Crustacea. Cirripedia 4. Group Echinodermata, Crinoidea BCREDP 9 (1985) F ROBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN 101 BOUNDARY NEAR MAASTRICHT Plate 16

1 2

0 mm 3 4 5 102 F ROBASZYNSKI ET COLL. BCREDP 9 (1985)

PLATE 17 MESOFOSSILS

Characteristic mesofossils from the ecozone 5. ENCi quarry. Maastricht

Fig. 1. Group Mollusca. Brachiopoda 2. Group Echinodermata. Ophiuroidea 3. Group Echinodermata. Asteroidea 4. Group Echinodermata. Echinoidea BCREDP 9 (1985) F ROBASZYNSKI ET COLL. CAMPANIAN-MAASTRICHTIAN 103 BOUNDARY NEAR MAASTRICHT Plate 17

1 2

4 3 0 mm 5 104 F ROBASZYNSKI ET COLL. BCREDP 9 (1985)

PLATE 18 MESOFOSSILS

Characteristic mesofossils from the ecozone 6. ENCi quarry, Maastricht

Fig. 1 Group Foraminifera. Siderolites 2. Group Porifera. Bryozoa

3. Group Crustacea. Decapoda 4. Group rest. Serpulidae BCREDP 9 (1985) ROBASZYNSKI ET COLL. CAMPANIAN-MMSTRICHTIAN 105 BOUNDARY NEAR MMSTRICHT Plate 18

1 2

3 4 0 mm 5 106 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 19 OSTRACODS

Smooth-shelled Ostracods from Vaals and Gulpen Formations at Halembaye (H) and Beutenaken (B)

Fig. 1-2. - Cytherella ex gr. ovata (ROEMER, 1841) 1 B 82-1 (1 a = dorsal. 1 b = left view) 2 H 82-1 (left view)

3-4. - Cytherella ex gr. contracta VAN VEEN, 1932 3 B 82-1 (right view) 4 B 82-2 (left view)

5-7 - Bairdia spp. 5 B 82-2 (right view) 6-7 H 82-1 (right view)

8. Sphaeroleberis sp. H 82-1 (8 a = left view, 8 b = interior)

9. Sphaeroleberis saccata (MARSSON, 1880) B 82-2 (9 a = dorsal, 9 b = right view)

10. Krithe vanveenae DEROO, 1966 B 82-2 (10 a = dorsal. 10 b = left view)

11-12. Asciocythere bonnemai DERoo, 1966 B 82-2 (11 a = left view, 11 b = interior. 12 a = dorsal. 12 b = right view) BCREDP 9 (1985) F. ROBASZYNSKI ET COLL. : CAMPANIAN-MAASTRICHTIAN 107 BOUNDARY NEAR MAASTRICHT: Plate 19

0.5 mm

11a0

, 121:>0 108 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 20 OSTRACODS

Ornamented Ostracods from Vaals and Gulpen Formations at Halembaye (H) and Beutenaken (B)

Fig. 1. Cytherelloidea cf. obliquirugata (JONES & HINDE. 1890) H 82-1 (1 a = dorsal. 1 b = left view)

2-3 - 5-6. Cytherelloidea levigata HERRIG, 1963 B 82-2 (left views)

4. Cytherelloidea sp. B 82-2 (4 a = dorsal. 4 b = left view. 4 c = right view)

7-9. Pterygocythere laticristata (BosauET. 1854) H 82-1 (7 a = left view. 7 b = interior. 8 a = dorsal. 8 b = right view. 9 a = right view. 9 b = interior)

10. - Aversovalva v-scriptum VAN VEEN. 1936 B 82-2 (10 a = dorsal. 10 b = right view) BCREDP 9 (1985) F. ROBASZYNSKI ET COLL. · CAMPANIAN-MAASTRICHTIAN 109 BOUNDARY NEAR MAASTRICHT. Plate 20

1a 2

4b 1b

4c 0.5 mm

Qb 110 F ROBASlYNSKI ET COLL. BCREDP 9 (1985)

PLATE 21 OSTRACODS

Ornamented Ostracods from Vaals and Gulpen Formations at Halembaye (H) and Beutenaken (B)

Fig. 1-3. - Veenia foersteriana ( BosauET. 1847) 1 H 82-1 (1a = left view, 1 b = interior) 2 H 82-16 (2 a = dorsal. 2 b = right view) 3 H 82-1 (3 a = right view. 3 b = interior)

4. Bythoceratina pedata (MARSSON, 1880) H 82-4 (left view)

5. Bythoceratina cf. longispina (BosauET. 1854) B 82-3 (left view)

6. Schizocythere aff. chelodon (MARSSON, 1880) H 82-8 (left view)

7-9. Amphicytherura? slenakensis DERoo. 1966 7 H 82-1 (7 a = dorsal. 7 b = left view) 8 B 82-3 (right view) 9 B 82-2 (left view)

10. Schizocythere aculeata ( BONNEMA, 1941) B 82-2 (right view)

11 Hemicytherura sp. B 82-3 (right view)

12-13. Mosae/eberis rutoti DEROO. 1966 12 H 82-6 (12 a = right view. 12 b = interior) 13 H 82-5 (left view) BCREDP 9 (1985) F ROBASlYNSKI ET C:J__ :.:.v:::.', .!.'.-V:..AS"1!CHTIAN 111 BOUNDARY ",iEAA v_.;;..5--:: c-- =-ate 21

�

� la 8

05mm 112 F ROBASZYNSKI ET COLL. BCREDP 9 (1985)

PLATE 22 OSTRACODS

Ornamented Ostracods from Vaals and Gulpen Formations at Halembaye (H) and Beutenaken (B)

Fig. 1. Pterygocythereis phylloptera (BosouET. 1854) B 82-2 (1 a = dorsal. 1 b = left view)

2. Pterygocythereis aft. tuberculata (VAN VEEN, 1936) H 82-1 (2 a = dorsal, 2 b = right view. 2 c = interior)

3. Planileberis parva ( BONNEMA, 1941) H 82-7 (right view) 4. Spinoleberis cf. pseudoeximia DERoo. 1966 H 82-12 (right view)

5. Phacorhabdotus batavus DEROO. 1966 H 82-1 (left view)

6. lmhotepia marssoni ( BONNEMA. 1941) H 82-12 (left view)

7-8. Curfsina cf. alseni CLARKE. 1983 7 B 82-2 (left view) 8 H 82-1 (8 a = left view, 8 b = interior)

9. Curfsina anorchidea {VAN VEEN, 1932) B 82-8 (left view)

10-11 Eucytherura dorsotubercu/ata VAN VEEN, 1938 10 B 82-2 (right view) 11 H 82-9 (right view) 12-13. - Cythereis spp. 12 H 82-2 (12 a = right view. 12 b = interior) 13 B 82-8 (left view)

14. - Cythereis hallembayensis DEROO. 1966 B 82-8 (left view) BCREDP 9 (19B5) 113

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