Detailed biostratigraphy of the SantoniadCampanian boundary interval in Northern Israel

A. ALMOGI-LABIN', Y. ESHET', A. FLEXER2, A. HONIGSTEIN1-2, S. MOSHKOVITZ' & A. ROSENFELD' 1. Geological Survey of Israel, 30 Malkhei Yisrael St., Jerusalem 95501, Israel

2. Dept of Geophysics and Planetary Sciences, Tel Aviv University, Ramat Aviv 69978, Israel

ABSTRACT - One of the best continuous and fossiliferous Late Santonian-Early Campanian successions in Israel is the approximately 6m thick Kabri section in northern Israel. Its chalky mark were deposited in an outer shelf to upper slope environment with minor depth fluctuations. This Santonian/Campanian interval was studied examining calcareous nannoplankton, palynomorphs, ostracods and benthonic and planktonic foraminifera. The planktonic foraminiferal Dirurinrllu usyrnrtricu - Glohoti.unc,unitu rlriwtu concurrent range zone was first observed in Israel in the Kabri section. The first occurrence of Aspidolithus purcus purcus herein is characterized by small specimens, difficult to determine by light microscopy. The lower boundary of the Campanian in this sequence was defined by the first occurrence of G. rlr i~utu, in accordance with the ammonite stage definition. This datum line nearly coincides with the first occurrence of the nannofosail marker A . puri'us parrus and with the base of the Lr,yurninoc,ythrrris tforsocostutu (S-4) ostracod ~oiie. both slightly above the foraminiferal boundary.

INTRODUCTION Coniacian-Maastrichtian sediments in northern Israel consist genemlly of rather homogenous chalky units (Mount Scopus Group; Flexer, 1968). The Late Coniacian-Campanian white chalks , up to 200m thick, are grouped into the En Zet im Formation. The Kabri Marl (Baida, 1964) is an intercalation within this formation, representing a clear marker in the uniform succession. It was re-sampled for this study in its type section at the quarry, 2km SSE of Kibbutz Kabri (coordinate 16518/26738, Israeli grid: Fig.]). This is the only known fresh exposure of this unit, which is generally covered by thin layers of soil or caliche. One sample ( A F 751; Fig.2) was taken from the underlying massive chalk of the En Zetim Formation near to the lithologic boundary, whereas nineteen samples were taken from the approximately six metres thick section of the Kabri Marl (AF 752- 770). This unit consists of soft chalky mark with minor shaly layers of yellowish-greyish colour. The upper boundary of the Kabri Marl with the overlying white chalks (AF 771-774) exhibits an irregular wavy contact with a dark greyish clay layer of about 2cm thickness at the contact (part of sample AF 771). The Kabri Marl section is very fossilifemus, with Gryplzaea i,esicdaris and S c , ~ / t r gor;\ti in its middle part: as well as Anc~u/i /c~s sp. at its top. The section was dated by foraminifera as Early Campanian (Baida, 1964). The aim of the present study is to reexamine the Santonian-Campanian interval of this section by means of multiple micropalaeontological methods.

MICROPALAEONTOLOGY Tucnty-four samples from the Kabri section were examined fo r thcir foraminifera, ostracod and calcareous nannoplankton content

(Figs 2-5). All contained assemblages of the three fossil groups. In addi t ion, f ish teeth, prisms of Znocerumus, coprolites and phosphatic grains were found in some washed residues. Three of the samples (AF 752, 771 and 774) were also palynologically analysed. Some significant fossils of each group are figured on Plates 1 and 2.

CALCAREOUS NANNOFOSSILS Nearly all samples were found to be rather rich in calcareous nannofossi ls and s o m e samples fo rm nanno-ooze . T h e assemblages are usually widely diversified and contain more than fifty species (Fig.2). Most of the species were already recorded in Late Cretaceous sediments of this part of Tethys (Moshkovitz, 1967, 1984, 1987; Shafik & St radne r , 1971; Naj i , 1983: Gvirtzman et a / . 1985, 1989; Reiss r/ al. 1985). The fossils in the Kabri section are rather well preserved, but in some samples recrystallization or etching is observed. The section can he divided into three nannofossil biozones (see Sissingh, 1977; Perch-Nielsen, 1979, 1985):

Samples AF 75 1-754: Lucianorhabdus cayeuxii (CC 16) Zone -

Samples AF 755756: Calculites obscurus (CC 17) Zone - Late

Samples AF 757-772: Aspidolithus parcus (CC 18) Zone - Early

Late Santonian

Santonian-earliest Campanian

(not earliest) Campanian

The biozonation of the highest samples, AF 773-774, is not clear.

39

A. Almogi-Labini, Y. Esheti, A. Flexer, A. Honigstein, S. Moshkovitzi & A. Rosenfeld

T E L A V l V

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Fig. 1 . Location Map.

The Lucianorhahdus cayeuxii (CC 16) Zone is the lowermost nannofossil zone in our section. Here, nannofossils are common and moderately or poorly preserved, showing some etching and recrystallization. The CC 16 Zone was defined by Sissingh (1977) as the interval from the first occurrence (FO) ofL. cayeu.r.ii to the regular FO of Ca1culite.s ohscurus. Only the uppermost part of this zone, (Late Santonian) is represented in the Kabri section. The assemblage is dominated by Watznaueria harnesue (PI. 1 fig.@, accompanied among others by Eiffellithus eximius, Aspidolithus ,furti\,us (PI. I , fig.2). Broinsonia dentutu (PI. I , fig. I ) , Mic,irla

d e c u s sa t a , T h o r a c o s p h a e r a s p p . , H e 1 i c o 1 i t h u s c u n ea t u .r , G a r t n e rag o a n t h o p h or u s , Lucian o rh a hdu s cay e u x i i , Lit h rap h id i t e s car n i o 1 ens i s , Prediscosphaera cretacea and Marthasterites furcatus.

This assemblage is overlain by the Calculites ohscurus (CC 17) Zone. The samples contain abundant coccoliths. The preservation of the fossils is, in general, poor to moderate, some etching or slight recrystallization is noted. The CC 17 Zone is defined as the interval between the regular FO of C. ohscurus to the FO of Aspidolithus parcus and as Late Santonian-earliest Campanian in age (Sissingh, 1977; Perch-Nielsen, 1985). The occurrence of C. obscurus in the Late Santonian (Sissingh, 1977, p.52; Doeven, 1983, pp.13, 24; but Campanian according to Perch-Nielsen, 1985, p.362) is confirmed also in the Kabri section. There, C . obscurus (PI.1, fig.15) occurs rarely, although it is present in most layers above sample AF 754. The dominating species in this zone are W. harnesae, E . eximius, P. cretacea and Thoracosphaera spp. These are accompanied by rare to few occurrences of A. furtivus, H. cuneatus, M . furcatus, Eprolithus floralis and Calculites ovalis. All these species are known in Santonian sediments from various parts of the world.

The Aspidolithus parcus (CC 18) Zone is the uppermost zone in our section. The samples contain abundant nannofossils and sometimes form nanno-ooze. The preservation of the fossils is usually good, although some etching and recrystallization is observed, especially in the lower part of this zone. The CC 18 Zone is defined as the interval between the FO of A. parcus and the LO of M. furcatus and as Early (not earliest) Campanian in age (Sissingh, 1977; Perch-Nielsen, 1979, 1985). Due to the lack of upper successive samples, its upper boundary in the Kabri section is not clear enough to accurately mark the LO of M . furcatus. The assemblage in our samples is dominated by W. harnesae, Zygodiscus spp., Thoracosphaera spp., E. e-t-imius and L. carniolensis. These fossils are accompanied among others by Arkhangelskiella specillata (PI.1, figs 7, 14), A. cymbijormis, A . furtivus, B , dentutu, R. anthophorus, A . parcus espansus (PI. I . fig.3), H . cuneatus, M . furcatus, Lithastrinus grilli (PI.1, figs 9, 17) and C. ohscurus. The most indicative Campanian nannofossil species Aspidolithus parcus parcus was found from sample AF 757 upwards. The specimens of this form in the lowest samples of the CC 18 Zone (AF 757-758) are about 5-6 microns in size (PI. I , figs 4-5) and difficult to determine by light microscopy. They attain an average size of 10-12 microns in the upper samples (e.g. AF 772; PI. I , figs 6, 13). thus confirming the evolutionary trend, as suggested by Lauer (1975). This species must be included in the genus Aspidolithus Noel arid not in Broinsonia Bukry. The latter genus, designated by the type-species B. dentutu (Bukry, 1969, P1.2, figs 1-3; Hattner & Wise, 1980, PIS, figs 6-8). has a tapering central cross and lacks the round pores in the central area (see PI. I , fig. 1 ). and is not appropriate for species such as purut.7. In the uppermost sample AF 774, forms already close to A . parc.rrs constrictus could be observed. Their subspecific designation. however, remains questionable. since their central area is somewhat wider (b/a ratio around 1.0, see Hattner et nl.. 1980: Wise, 1983). Samples higher up might provide more information on the evolutionary lineage of the As~idolithits-Br.oi~~.~orii~/ group along the Santonian-Campanian boundary interval (see suggestions and discussions in Lauer. 1975: Perch-Nielsen, 1979:

oh li q u u m , R e in ha rdt i t e s

40

Detailed biostratigraphy of the Santonian/Campanian boundary interval in Northern Israel

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FlBUNDRNCE

PRESERUGTION IGENEROLI

PRESERUFlTION i H O D E l

a h m u e r e l l a o c t o r a d i a t a

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I I ~ z f f e l l x t h u s ex lmLus

I I E ~ f f e l l ~ t h u s t u r r i s e x f f e l i I I G a r t n e r a g o o b l ~ q u u m I I H a q i L l s ci r c V m r a d l d t u s I I H e 1 icol i T h U 5 cuneatc is I I K a m p t n e r i u s m a g n i f l c u s I I ~ l t h r a p h x d r t e s c a r n t o l e n s i s

I I L u c ~ a n o r h a b d u s caqeuwx 1

I I W a n ~ u x t e l l a pemmafoidea

I H a r t h a s t e r l t e s f u r c a t u s I I H 1 C Po rhabdlJ 1"s deco P a t U S

I I n a c u l a d e c u s s a t a

11 II P a ~ h a b d o l ~ t h u s e m b e r g e r i

I1 11 F r e d i s c o s p h a e r a c r e t a c e a II 11 Quadrum sp. I1 11 R e l n h a r d t i t e s d n t h o p h o r u s I1 11 Rhagod iscus a n g u s t u s I1 II StoUePilJS blaPCUS I1 II ~ h n r a c o s p h a e r a s p . l . ~ n o p o r e s ' I 1 11 Tho racosphaera sp .2 0 few p o r e s , II 11 T r a n U l i t h U S O r l ~ l ? a t U S I, II Ua tZnaUec ia ba rnesae II I1 Z q g o d ~ s c u s compactus I1 I1 Zqgodiscus dip logrammus I1 11 Z y q o l t t h u s c r u x ,I I1 R U C ~ n o l i t h U S h a q i i II 11 I1 U a g a l a p i l l a matalosa

II C q l ~ n d r a l z t h u s s e r r a t u s I1 11 II He te romargxna tus s ~ .

11 Pon tosphaera m u l t i c a r l n d t a I1 II Zqgod iscus s p . 8 l a r g e i I1 I1 C4spzdol i thus f u r t i u u s I1 II C4spido l iThus p a r c u s ewpan=us II II C a l c u l l t e s oua113 I, I1 E p r o l i t h u s f l o P a 1 1 4 11 11 U a t z n a u e r ~ a h x p o r t a I1 11 B raa rudnsphaera sp. I1 II C a l c u l l t e s o b s c i ~ r ~ s I1 I1 A S p i d ~ I i t h ~ ~ p a r c u s p a r c ~ i s I1 II C h i a s t o z q g u s 1 ~ t t e r a r , ~ ~ ,I 11 L i t h a s t r z n u z . grill, I1 II Scampdne l l d c u r n u t a I1 II r r e t a r h a h d u s C U ~ I C U S I, I1 R e l n h a r d t t t e s l e u i s II I1 Rhagodiecr ls asper II II T r a n n l 1 t h u s g a b a l u s II 11 B I S C ~ J ~ U ~ b l a c k 1 1 I1 11 H e x a l l t h u s g a r d e t a e

F'ig.2. Distribution chart of calcareous nannofossils in the Kabri Marl section

41

A. Almogi-Labini, Y. Esheti, A. Flexer, A. Honigstein, S. Moshkovitzi & A. Rosenfeld

Hattner et a l . , 1980; Crux, 1982; Wise, 1983; Stradner & Steinmetz, 1984). Marthasterites furcatus (P1.1, figs 11-12) is also an important species, its LO is known to occur in the early Campanian, somewhat above the FO of A. parcus parcus. In our section, M . furcatus is found up to sample A F 772. Hexalithus gardetae, another indicative form for the Campanian stage (Perch- Nielsen, 1985, p .390) is found in sample A F 771 . Large specimens of Helicolithus (=Chiustozygusj cuneatus (Lyu'leva) Cepek & Hay (PI. I , fig. 16) are rare in the Kabri section, but occur together with A . parcus parcus. T h e species differs from Eiffellithus traheculatus (Gorka, 1957) of Albian-Maastrichtian age (Thiers te in , 1976, p .339) by i ts larger form and the symmetrical cross. These forms usually accompany the Santonian nannofossil assemblages in central and southern Israel (Gvirtzman et ul. 1985, 1989), where they occur below the FO of A . parcus parc.us. A similar occurrence of large H. cuneatus was recorded in Early Campanian sediments from Site 51 1 in the South Atlantic - DSDP Leg 71 under the species name Eiffellithus traheculatus (Wise, 1983, p.491).

PALYNOLOGY Only a few, non indicative dinoflagellate cysts were found in samples AF 752 and 774. Sample AF 771 contains Manumiella spp. and some other poorly preserved dinoflagellates. Terrestrial plant particles, such as cuticles tracheids and inertinites, are relatively common in this sample. The occurrence of many fungal cells (Pl.1, figs 19-21), originating on land, is noteworthy.

OSTRACODS Ostracods are generally common to rare in the samples, only sample AF 754 yields abundant ostracods. The assemblages are relatively highly diversified and twenty-seven species, belonging to eighteen genera, were observed (Fig.3; for taxonomy see Honigstein, 1984). The section can be subdivided into three parts:

the S-3 ostracod Zone (AF 751), the S-3b Subzone (AF 753-757) and the S-4 Zone (AF 758-774).

The exclusively Santonian species Cythereis cretaria occurs only in the lowermost sample and indicates, together with Limhurgina miarensis and Cythereis cretaria dorsocauduta, the L. rniarensis (S-3) a s semblage zone of La te Santonian age (Honigstein, 1984; Honigstein et a/., 1987). Occurring above this level and upwards are, among other species, Cytherella aff. eliotti, Krithe solomoni (P1.2, fig. 14) and Bythocypris aff. howchiniana, which appear in the subzone S-3b of the hitherto undefined Santonian-Campanian boundary interval (see references above).

T h e samples A F 758-774 belong to the overlying Leguminocythereis dorsocostata (S-4) assemblage zone. The lower boundary of this zone in the Kabri section is defined by the FO of P. campania. Juvenile forms of this species were found from sample AF 758 upwards, already showing the development of subanterior ribs, typical for P. campania (Honigstein, 1984, p.17). Adult forms of P. campania (P1.2, fig.12) occur together with L. dorsocostata (P1.2, fig.11) from sample A F 76.5 and upwards. Eucytherura tetracornis (P1.2, fig.13) ranges in this section from AF 758 and upwards within the S-4 Zone.

FORAMINIFERA The foraminifera1 assemblage composition in the Kabri marl section was first investigated by Baida (1964). Most of the species determined are benthonic foraminifera and several of them were left in open nomenclature. Only five planktonic foraminifera1 species were recognized in the section. The Early Campanian age determination (Baida, 1964) was based only on general ranges of the fauna and should be re-evaluated.

The present study shows that benthonic and planktonic foraminifera dominate the >63 microns size fraction in our samples (Figs 4, 5) . The species are usually well preserved. The planktonic foraminifera are more abundant than the benthonic

Explanation of Plate 1

Calcareous nannoplankton and palynomorphs from the Kahri section (scale bar for figs 1-18, lpn for figs 19-21, l o p , )

Fig. I .

Fig.2.

Fig.3. Fig.4.

Fig.S.

Fig.6.

Fig.7.

Fig.8.

Fig.9. Fig. 10. Fig. I I,

Fig. 12. Fig.13.

Fig. 14.

Fig. IS Fig. 16.

Fig. 17.

Fig. 18.

Figs 19-21

42

Rroinsonia denruru Bukry, dorsal view, SEM micrograph, sample AF-766 (CC 18 Zone). Aspidolithus furriws (Bukry) Perch-Nielsen, dorsal view, SEM, sample AF-766 (CC 18 Zone). Aspidolirhus parcus e.xpansus (Wise & Wattkins) Perch-Nielsen, dorsal view, SEM, sample AF-758 (CC 18 Zone). Aspidolirhus parc'us parcus (Stradner) Noel, dorsal view. SEM, sample AF-757 (CC 18 Zone). A.Spid(J/ithU.Y pnrcus parcus (Stradner) Noel. dorsal view, SEM, sample AF-7.58 (CC I8 Zone). Aspidolirhus parcus parcus (Stradner) Noel. dorsal view. SEM, sample AF-772 (CC 18 Zone). Arkhangelskiella specillam Vekshina, dorsal view, SEM, sample AF-766 (CC 18 Zone). War;naurriu hurnesur (Black) Perch-Nielsen, coccosphere. SEM, sample AF-77 I , CC I8 Zone). Lithasrrinus ,grilli Stradner, top view, SEM, sample AF-766, (CC 18 Zone). Stovrrius hiarcus (Bukry) Perch-Nielsen, side view. SEM, sample AF-766 (CC 18 Zone). Marrhasrei-ires furcutus Deflandre, SEM, sample AF-7.58, (CC 18 Zone). Mur-rho.srrrir(~s fu r -mus Deflandre, LM. Pol. photograph, sample AF-770 (CC I8 Zone). A.sprdolithu.s/~urcrr.s purcu.s (Stradner) Noel, distal view, LM. Pol.. sample AF-771, (CC 18 Zone). Ai-khan,qc/.skirl/u sp,c.ilIara Vekshina. proximal view, LM. Pol., sample AF-761 (CC 18 Zone). Calculires / J / N U ~ U S (Deflandre). Prins & Sissingh, LM. Pol., sample AF-7.56 (CC 17 Zone). Helicolirhus (=Chiusroz?;gusJ cunearu.s (Lyu'leva) Cepek & Hay, LM. Pol., sample AF-770 (CC I8 Zone). Lirhastrinus

Detailed biostratigraphy of the SantonianKampanian boundary interval in Northern Israel

43

PP

w

m....................... ..................... ......=......=.......... ...../-...m.=....... .....m.....m..=.m....... ......-.=..-,-..... .=...-..-.m..m..m.... ...... ,=.I.. .. .-. .I.. .. .....-...-.-... ......-..... .m.-.-. *. .-. . .-. . .r-.-. .. .=...-.... .\-I. .-. .. -. . .-. .. .I-. .. ........m.....=..m.=.=.. .m....=..m.m.-.-.. .... .-. .-.=.-.-;. . .........=..-.-.m. ...................... . .=. .-. .=.=.=. .=.=.=. .-. ...-.-....l-.m. ..m ..........=...=.-.-...= .-’ ........................ ,......~......~.~...~ ........................ ‘D. ‘I-*-*-

.....mi-.-.=. .. m-

Fig.3. Range chart of ostracods in the Kabri Marl section.

although slightly decreasing in abundance in the upper part of the section where the benthonic species are more frequent and the faunas are rather poorly preserved. Most of the planktonic species belong to the genera GlohiRerinelloides, Hedherge l la and Heterohelix (Fig.4). Globotrucanids are diversified and common, but represent only a minor componen t of t he planktonic foraminiferal assemblage. Twenty Globotruncanidae species were identified throughout the section, the maximal diversity of this family is observed in its middle part (fifteen species, sample AF 767). The ranges of Globotruncanidae species enable a division of the Kabri Marl section into three planktonic foraminiferal zones which are in accord with the Tethyan zonation (Kuhry, 1970; Barr,

1972; Wonders, 1980; Dowsett, 1984; Robaszynski et a/.. 1984). The lower Dicarinel la asyrnetrica interval zone (Late

Santonian) is determined by its index fossil (P1.2, figs 5-6) as from the base of the succession up to the FO of Glohotluncanita ele\.trru (P1.2, figs 8-9) at sample AF 755. From this sample up to sample AF 768, D. asyrnetriru and G. r le~nra occur together and define the D . a.7ymrtric.a - G. Elei.ata concurrent range zone. This zone was hitherto not observed in Israel (Reiss et al., 1985; Almogi- Labin et a / . , 1986; Honigstein et a / . , 1987). The overlying G. elevata interval zone (Early Campanian) starts above the extinction of D . asymutric.~ and ranges from sample AF 769 to the top of the section.

44

A. Almogi-Labini, Y. Esheti, A. Flexer, A. Honigstein, S . Moshkovitzi & A. Kosenfeld

C r i s t ae 1 eb e r i :B Cqthereis cretaria Cqthereis cretaria dorsocaudata Cqthereis mesa mesa Cqthereis rosenfeldi eUolUta Cqtherella cf. austinensis Limbutgina miarensis Oertl iel la? cf. rasbaalbekensis Bairdoppilata pondera Cqtherel loidea israelidna Spinoleberis megiddoensis

Brachqcqthere cf. ekpo Buntonid? af f . cretaizea Cqtherella aff. eliotti Brachqcqthere angulata Bqthocqpris af f. howchiniana Cqthereis diuerseveticulata C q t he r 1 i s mesa ue n t r o r e t i c:u 1 at a Krithe solomoni Bqthocqpris windhami Cristaeleberis fopnicata Went r o c q t he re i s Eucqtherura tetracovnis P r.0 to t n u n ton i a camp an i .a Ptetqgocqthereis sp . Legum i nocqthe r e i s dorsocostata

r e t i cu 1 a t .3

e; i na i ens i s

Phac:othaldotus cf. inaequicostatus

Detailed biostratigraphy of the Santonian/Campanian boundary interval in Northern Israel

- lmluALn-- I I .m.. . . . . m . . . . . . . . . . . . . . . . . . . . . . . m * r n a a

EIIII.~-~ . . a............... m . m . m . . . . . . . . . . . . . . . . . -.-.a. . . . . . . - . . ~ . - . - . . . . . . . . . . . . . . .

-L

I= =- .m. .-. .-.-.-. . . . . .=.-.=.a.m. .-. .m.. ..m.............m....... . . m . . . . m . . . .m. i . - . . . . . . . .c-u.-.i--. . . .m. . . . . . . m . m . . . . . . . m . . . . . m . . . . . . . - . . . . - . . . - . . . . . . . . . . . . . m . . .-. . i - ~ . . . . . . . . . . . . . . ~ . ~ . . ~ . ~ ................I.-

. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

i II II II H W I I II I H I I I

Y

H

n

n n n n n n n n n n n n n n n

I

Y

Y H I I

I II II Y

n

Fig.4. Distribution chart of selected planktonic foraminifera in the Kabri Marl section.

]Besides these species the first and last occurrences of the following planktonic taxa are noteworthy: the LO of Dicarinella conlravata in our samples is found within the lowermost D. asymetrica Zone, together with the FO of Glohotruncana hulhides and G. rnariei. The FO of Glohotruncana arca (P1.2, fig. 10) and Glohotruncanita stuartiformis is recorded in the overlying samples of the D . asyrnetrica - G . elevata Zone. A gradual turnover from Marginotruncana species dominated faunas into assemblages composed mainly of species of Glohotruncana and Glohotruncanita is observed within this zone. The LO of several species of Marginotruncana is observed in this interval. M. coronata disappears first, then M . angusticarinata and M . ta$ayaen.sis, followed by M . pseudolinneiana (P1.2, fig.4) and M . sinuosa. The LO of M . undulata (P1.2, fig.7) is recorded close to the base of the G. elevata Zone (AF 769). The ranges of most of these Murginotruncana species in Israel (Almogi-Labin et a / . , 1986) must therefore be extended into the D. asymetrica - G . rlcvatu Zone.

The benthonic species, depicted in Fig. 5 , add information to the planktonic assemblages. Within the D . asymetrica - G. elevata Zone the FO of several benthonic foraminifera index species is recorded. Gwoidinoides pseudosimiensis (P1.2, fig.2) occurs at the

Dicarinella asqmetrica Dicarinella concauata Globotruncana linneiana Harginotruncana angusticarinata Harginot runcana coronata Harginotruncana sinuosa Marginotruncana tarfaqaensis Rosita fornicata Ma rgi not runcana ma rg i nata Uentilobrella glabrata Globotruncana bulloides Globotruncana mariei Uentilrbrella eggeri Globotruncanita eleuata Globotruncanita stuartiformis Marginotruncana pseudolinneiana Marginotruncana undulata Rosita sp. Globotruncana arca Globotruncana cf. orientalis Marginotruncana sp. B Globotruncana austinensis

base of this zone, Anornalinoides sernicornplanata (Pl.2, fig. 1) at its middle part and Neofahellina rugosa (P1.2, fig.3) from sample AF 766 upwards.

PALAEOENVIRONMENT The Kabri Marl sequence represents one of the best, well- preserved, and continuous Late Santonian-Early Campanian sections in Israel. Their floral and faunal content indicate deposition in an outer shelf to upper slope environment with minor fluctuations. The foraminifera1 assemblage is dominated by planktonic species. The large species of the Globotruncanidae are well diversified. The ostracod assemblages, in general, indicate a warm (Cytherelloidea), outer shelf environment with minor changes to greater water depth (Krithe). The nannofossil and foraminifera assemblages show a somewhat deeper environment of deposition in the middle part of the succession (nanno-ooze), whereas in the lower and upper parts of the section a relative shallowing is suggested. This shallowing trend in the upper part of the section (AF 770 and upwards) was observed also by the increase in benthonic foraminifera and the decrease in the number of Globotruncanidae species. In this interval, ostracods are generally rare and lack the deeper water species Krirhe solornoni.

45

A. Almogi-Labini, Y. Esheti, A. Flexer, A. Honigstein, S. Moshkovitzi & A. Rosenfeld

p -J -J -1 -.I -1 -.) -J -.J -J -.J J -.J -.J -.J -.J -.J -.J -.J -.J -.] -J -.J -J -.J u1 Lrl LII UI 0 Lrl Lrl LO Lrl D- 0- D. p 0. 0- 0. 0. 0- 0- -J -J -J :J -.J + 1.3 CJ P LII 0- -J m Q -3 + t..i I,I P u rr J m Q o + t..i 121 P

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. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

Fig.?. Distribution chart of selected benthonic foraminifera in the Kabri Marl section.

.I n I Rlabamina sp. I I1 Rnoma 1 i no ides sp. R R Gaudrqina sp. H II Globorotalites subconica W H Gqroidinoides sp. U II Neoflabellina sp. H I Spiroplectammina laeuis n II Gqroidinoides pseudosimiensis R U Quadrimorphina allomorphinoides n H Tritaxia gaultina I U Gaudrqinella pseudoserrata H I Rnomalinoides semicomplanata H II Dorothia sp. n H Neoflabellina rugosa H II Bolivinoides pustulata n I( Pseudogaudrqina pqramidata U II Siphogaudrqina stephensoni

Explanation of Plate 2

Foraminifera and ostracods from the Kabri section

Fig. 1 Annniulinnidrr srmic~omplanutu (Cushman & Hedberg), lateral view, sample AF-769 (G. rlrwru Zone). Fig.2. Gyroidinoidex pseudo.simirnsi.s Reiss, umbilical view, sample AF-767 ( D . o.pww/rrcu - G. c ~ l ( w ~ t u Zone). Fig.3. Neoj7uhrllinu I - u ~ o s u (d’orbigny), sample AF-770 (G. elrimu Zone). Fig.4. Marginnrruncunu pseudolinneiunu Pecsagno, umbilical view. sample AF-767 ( D u.syrrrrrir u - G rlci~utu Zone). Fig.?. Dic~urrnellu us,vmrtrrc~u (Sigal), umbilical view. sample AF-761 ( D . a.synctric.u - G. c~lci~crru Zone). Fig.6. Diwrinellu u~ynrtr ic~u (Sigal), lateral view. sample AF-763 ( D . u.cynic~ic~a - G. clei,utu Zone). Fig.7. Mar~inorrunc,uno unduluru (Lehmann), umbilical view, sample AF-763 ( D . u.rynierric,u - G. olcvuru Zone). Fig.8. Glnhotruncunitu rlewita (Brotzen). lateral view, sample AF-764 ( [ I . uswnetr-icw - G. rlei.utcr Zone). Fig.9. Glohotrunc.unitu Fig. 10. Gloho/runcwm UJTU (Cushman). umbilical view, sample AF-770 (G. i~leiutu Zone). Fig. 1 I . Lc,yuminoc~~therf,;.s ~ O I - . S O ~ O S I U I U Honigstein, right view, sample AF-765 (S-4 Zone). Fig. 12. frorohuntoniu cumpuniu Honigstein, left view, sample AF-766 (S-4 Zone). Fig. I ? . Euc.yrher-ura trrruc.ornis Honigstein. right view, sample AF-760 (S-4 Zone). Fig. 14. Krithr solonroni Honigsteiii, right view. sample AF-766 (S-4 Zone).

UIU (BrotLen), umbilical view, sample AF-761 (D . asvmctriiu ~ G r/eiwtu Zone).

46

Detailed biostratigraphy of the SantonianKampanian boundary interval in Northern Israel

41

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Detailed biostratigraphy of the Santonian/Campanian boundary interval in Northern Israel

The relatively abundant terrestrial plant particles in sample AF 771 suggest a nearby landmass, serving as a source, at that time. This is supported by the relatively poor buoyancy of these particles, which could not have been transported by currents over a great distance..

THE SANTONIAN/CAMPANIAN BOUNDARY The stage boundary between the Santonian and the Campanian was defined by the first occurrence of the ammonite Placenticeras hidorsaturn (de Grossouvre, 1901; Haug, 191 I ) . The calcareous nannofossil Santonian/Campanian biostratigraphy was studied by Stover (1966), Manivit (1971), Thierstein (1976), Sissingh (1977), Verbeek (1977) and Lambert (1981). The first occurrence of Aspidolithus parcus was regarded by some authors as the base level of the Campanian (Manivit, 1971 ; Thierstein, 1976; Verbeek, 1977). Others placed its first occurrence somewhat higher and not in the earliest Campanian (Sissingh, 1977; Perch- Nielsen, 1979, 1985; Lambert, 1981). Likewise, the same was suggested because of the position of the first occurrence of A . pa rcus above the top of the magnetic anomaly 34 at the Santonian/Campanian boundary (Stradner & Steinmetz, 1984; Monechi & Thierstein, 1985).

The foraminiferal biostratigraphical biozonation in the boreal and Tethyan regions is mainly based on the ranges of D . trsymetr~ica and G . e l eva ta , which allow for different interpretations. The Santonian/Campanian boundary is usually placed either at the last occurrence of D. asymetricu (Wonders, 1980; Robaszynski et al., 1984; Marks, 1984; Caron, 1985; Reiss et al,, 1985; Almogi-Labin et al., 1986; Niter, 1989) or at the first occurrence of G . elevatu (Premoli Silva, 1977; Sigal, 1977; Weidich, 1984; Wagreich, 1988). Other foraminifera species, such as G. arca and N . riigosu were also used to mark this stage boundary (e .g . Birklund et al., 1984).

In Israel, the last occurrence of the common foraminiferal species D. asyrnerricu is generally used as the main marker of the Santonian/Campanian boundary (Reiss et a l . , 1985, 1986; Almogi-Labin et al., 1986; Honigstein et al., 1987; Gvirtzman et ul., 1989). The occurrence of the other above mentioned index foraminifera is rather rare and sporadic at this level. In many Israeli sections an undefined interval separates the last occurrence of D . asyrnetrica and the first occurrence of G. a r m and G. clevata (Honigstein el a l . , 1987). Diagnostic planktonic foraminifera are absent in this interval. The nannofossil marker A . par-cus was defined in Israel as Early (not earliest) Campanian in age (Gvirtzman et al . , 1989). The lower boundary of the L. iiorsocostuta (S-4) ostracod assemblage zone generally marks the Santonian/Campanian boundary. The S-3b Subzone was hitherto defined only as Santonian/Campanian in age (Honigstein, 1984; Honigstein et al., 1987).

In the Kabri Marl section, the Santonian/Campanian boundary is defined in a multidisciplinary framework by nannofossils, foraminifera and ostracods (Fig.6); index ammonites are absent.

A combined study (ammonites. foraminifera and nannofossils) in the Gosau area, Austria, revealed that an ammonite, similar to the stage marker f . hidorsatum was found together with the D. ,4syrnetrica - G. eleiwta concurrent range zone and below the first occurrence of A. parcus (Wagreich, 1988). This ammonite (P. cf. hidorsatum; see Summesberger, 1979, 198.5) is poorly preserved,

but belongs, according to W.J. Kennedy (written comm., 1990), to P. hidorsaturn. In Israel, age indicative ammonites were hitherto not observed at this level.

In the Kabri section, D. asyrnetrica and G. elevuta were also found concurrently. In accordance with the stratigraphic position o f f . hidorsaturn and its correlation with the first occurrence of G. elevata in the Gosau area (Wagreich, 1988), the boundary in the Kabri section must be determined by the first occurrence of G. elevata in sample AF 755. Accordingly, the former foraminiferal stage determination in Israel and the Tethyan region must therefore also be corrected. The gradual overturn of the foraminiferal assemblages occurs thus mainly within the Early Campanian. The first occurrence of A . purcus parrus in sample AF 757 is found within the Early Campanian foraminiferal D . asyrnetrica - G. elevata Zone and indicates a position very close to the base of the Santonian-Campanian boundary. The base of the Early Campanian L. dorsocostatu (S-4) ostracod zone at sample AF 758 is located about Im above the foraminiferal Campanian boundary and about 40cm above the first occurrence of A . purcus p a r c u s . The age of the underlying S-3b Subzone is now determined as latest Santonian-earliest Campanian. The datum lines of the different biozones, referring to the Santonian- Campanian boundary, are located within the lower part of the Kabri Marl section and nearly coincide.

ACKNOWLEDGEMENTS The authors wish to thank Dr W.J. Kennedy, Oxford

University, U.K., for his comments on the Gosau ammonite definition. They also thank Bevie Katz for editing the manuscript, Tamara Beer and F. Calafateanu for preparing the samples, and M. Dvorachek and Y,. Levy for the SEM and light microscopy photographs. The latter are all from the Geological Survey of Israel, Jerusalem. Manuscript received February 1990 Revised manuscript accepted November 1990

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50