STATE OF ISRAEL :: :

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■ UPPER CALLOVIAN AMMONITES( ’ , AND MIDDLE JURASSIC GEOLOGICAL HISTORY OF THE MIDDLE EAST

Zeev Lewy

GEOLOGICAL SURVEY of ISRAEL

BULLETIN 76

I Jerusalem , August 1983 STATE OF ISRAEL

MINISTRY OF ENERGY AND INFRASTRUCTURE GEOLOGICAL SURVEY OF ISRAEL

BULLETIN

ISSN 0075-1200

GEOLOGICAL SURVEY OF ISRAEL 30 Malkhei Israel St., Jerusalem 95 501, Israel Editorial Board

Chairman: R, Bogoch Managing Editor: B. Katz Z.B. Begin, A. Ehrlich, A. Sneh, G. Steinitz Layout: A. Peer, S. Levy UPPER CALLOVIAN AMMONITES

AND MIDDLE JURASSIC GEOLOGICAL HISTORY

OF THE MIDDLE EAST

Zeev Lewy

Geological Survey of Israel

August, 1983 CONTENTS

ABSTRACT 1 INTRODUCTION 3 PROVENANCE OF MATERIAL AND DEPOSITION 3 STRATIGRAPHY 5 REVISED MIDDLE JURASSIC STRATIGRAPHY OF THE MIDDLE EAST 7 I. Ammonite Assemblages 7 II. Chronostratigraphy 7 (a) Previous works (b) Revisied Middle Jurassic ammonite chronostratigraphy (c) Remarks on microfaunal chronostratigraphy (d) The boundary between the Lower and the Upper Zohar Formation III. Stratigraphic Correlation With Adjacent Regions 10 (a) Saudi Arabia (b) Lebanon and Syria (c) Abu Darag Region, Eastern Egypt (d) Zerqa River, Jordan THE NATURE OF THE UNCONFORMITY 12 GEOLOGICAL HISTORY 13 SYSTEMATIC PALEONTOLOGY 15 ACKNOWLEDGEMENTS 39 REFERENCES 40

LIST OF FIGURES

1. Location map 2 2. Columnar section of Jurassic rocks in Israel 4 3. Bullatimorphites bullatus (d'Orbigny) 5 4. Ammonite whorl sections 47 5. Ammonite whorl sections 49 6. Ammonite whorl sections and sutures 51 7. Jurassic ammonites in Makhtesh Hatira 52 8. Jurassic ammonites at Gebel El-Minshera 53 9. Mid-Jurassic ammonites in Israel and Sinai 54 10. Corellation of Jurassic formations 55 11. Generalized revised corellation 56

PLATES 1 - 8

UPPER CALLOVIAN AMMONITES

AND MIDDLE JURASSIC GEOLOGICAL HISTORY

OF THE MIDDLE EAST

ABSTRACT

Ammonites from the Jurassic outcrop at Makhtesh Hatira (Kurnub anticline, Israel) were studied and compared to coeval ammonites recently collected at Gebel Maghara and Gebel El-Minshera (northern Sinai, Egypt). Forty species are distinguished, including a new genus, seven new species and thirteen unnamed ones. The ammonites are divided into two assemblages, both recognizable at Gebel El-Minshera and at Makhtesh Hatira, whereas at Gebel Maghara, only the Upper Assemblage occurs. Both assemblages are attributed to the Upper Callovian; the Upper Assemblage belongs to the Lamberti Zone and part of the Lower possibly ranges into the upper part of the earlier Athleta Zone. Because of the absence of typical cardioceratine ammonites the distinction of the boundary between these two European biozones is quite impossible in southern Tethyan regions. Therefore, both assemblages are attributed to the combined Athleta-Lamberti Zone. Poorly preserved, fragmentary specimens found in the Lower Assemblage which resemble Middle Callovian ammonites are discussed. On the basis of biostratigraphical and lithofacies considerations, a Late Callovian age is attributed to the whole Upper Zohar Formation in the northern Negev, Israel. The Upper Zohar Formation unconformably overlies the Lower Zohar Formation in whose upper part the Meyendorffina b a th on ica Assemblage Zone occurs. This biozone was previously attributed exclusively to the Late Bathonian, but it is herein suggested that it ranges into the Early Callovian. An Upper Bathonian-Upper Callovian unconformity is suggested to occur within the Atash Member of the Upper Dhruma Formation in central Saudi Arabia, based on a revision of the Middle Jurassic ammonites and accompanying faunas recorded from there.

Isr. Geol. Surv. , Bull. No. 76 pp. 1-56, 11 Figs; 8 Pis. Jerusalem, August, 1983

GSI Bull. 76, 1983 1 LEWY U. CALLOVIAN AMMONITE;

Figure 1. Location map of Jurassic outcrops and selected drillholes which penetrated rocks of this stage in Israel and adjacent countries (modified after Goldberg and Friedman, 1974

GSI Bull. 76, 198 2 U. CALLOVIAN AMMONITES Z. LEWY

INTRODUCTION 1968; Hirsch, 1980) and Echinoidea (Parnes, 1961). Similarly, the ammonites collected at Gebel The Mid-Jurassic outcrop at Makhtesh Hatira El-Minshara enabled revising the ages given to the (Kurnub anticline), Israel, is one of a few Jurassic rocks there by Farag and Shata (1954) and well-exposed and highly fossiliferous Jurassic Farag and Omara (1955). The present study rock-sequences in the Middle East, similar in this resulted in the proposal of a new ammonite respect to the exposures at Gebel Maghara, biostratigraphy, assigning new ages to the Jurassic northern Sinai, Egypt and Gebel Tuwaiq, Saudi rock-units of Makhtesh Hatira, as well as a Arabia. The stratigraphy of these three outcrops revision of the Jurassic stratigraphy of Gebel has been thoroughly studied by geologists and Tuwaiq (Saudi Arabia) and Abu Darag (Egypt). paleontologists (Gebel Maghara: e.g. Douville', The present study was conducted parallel to 1916; Al-Far, 1966; Goldberg et al., 1971; Gebel G. G ill, H. Tintant and J. Thierry's work on Tuwaiq: e.g., Arkell, 1952; Powers et al., 1966; ammonites from the same section, and presents a Imlay, 1970; Kier, 1972; Makhtesh Hatira: e.g., different biostratigraphy from that of Gill and Hudson, 1958; P&rnes, 1961; Goldberg, 1963; Tintant (1975). Preliminary biostratigraphic Reiner, 1968; Hirsch, 1980), contributing to the conclusions of the present study were published by knowledge on the Jurassic stratigraphy and facies the author (Lewy, 1981, 1981a) and are in part changes of the rock-units in which oil reservoirs amended herein. were discovered in adjacent areas. In 1975, Gill and Tintant briefly recorded thd ammonite biostratigraphy of Makhtesh Hatira, changing the chronostratigraphy of Hudson (1958), which was based on a few ammonites (determined by L.F. Spath), Bivalvia and Gastropoda (determined by L.R. Cox), Brachiopoda PROVENANCE OF MATERIAL (determined by H.M. Muir-Wood), some corals AND DEPOSITION (determined by F. Gosling) and other groups such The ammonites studied were found in the as Foraminiferida and Stromatoporoidea. In their Jurassic outcrop at Makhtesh Hatira (Kurnub distribution chart, Gill and Tintant (1975) noted anticline) from 9 m above base Tsia Member the coexistence of the genera Thamboceras (subunit 6 of Goldberg, 1963) of the Upper Zohar (Upper Bajocian), Erymnoceras (Middle Callovian) Formation, throughout the overlying Kidod and P a ch ycera s (Upper Callovian). This Formation and in the following 20 m of the biostratigraphic discrepancy stimulated the Be'er Sheva Formation (Gill and Tintant, 1975, present study of the ammonites of Makhtesh recorded ammonites up to 50 m above the base Hatira in the material at the Geological Survey o f this formation). Another single finding was of Israel, collected by M. Raab during the study of from the top of the Be'er Sheva Formation. the Jurassic sequence by Goldberg (1963). The ammonites at Gebel Maghara occur in a Additional material was found by F. Hirsch, L. single unit, 1-10 m thick, at the top of the Picard and the author. Some Callovian ammonites Zohar Formation (subunit 82 of Goldberg et al., were recently collected at Gebel Maghara and 1971). The ammonites at Gebel El-Minshera’‘occur Gebel El-Minshera, northern Sinai by the author along the upper 17 m of the sequence and accord with a few additional specimens by Y. Bartov, Y. a litho- and biostratigraphic correlation to both Druckman, R. Freund and F. Hirsch. These Gebel Maghara and Makhtesh Hatira. Callovian ammonites are incorporated into a Sample numbers of the ammonites deposited regional Callovian ammonite biostratigraphy and in the collections of the Geological Survey of compared to the assemblages recorded from Saudi Israel are prefixed by M-; those from the Arabia (A rkell, 1952; Imlay, 1970) and Egypt collections of the Hebrew University of (Abdallah et al., 1S65). The chronostratigraphy as Jerusalem by HU-. The number of specimens based on the ammonites is herein correlated with within a sample is given in brackets and the the ages attributed to the same rock units in individual specimen number within a sample (if Makhtesh Hatira and northern Sinai on the basis more than one) is given after a colon. Forty of calcareous nannofossils (Moshkovitz and ammonite species are described and illustrated Ehrlich, 1976; 1981), Foraminiferida and Ostracoda including a new genus, seven new species and (Maync, 1966), Bivalvia and Gastropoda (Reiner, thirteen unnamed ones.

GSI Bull. 76, 1983 Z. LEWY U. CALLOVIAN AMMONITES

Figure 2. Schematic composite columnar section of the Middle to Upper Jurassic rock sequence in southern Israel (modified after Goldberg, 1970).

4 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

STRATIGRAPHY Formation and the lower part of the overlying Sherif Formation (as determined by Goldberg et The stratigraphic position of the ammonites a l, 1971) exposed at Gebel Maghara, northern studied is in accordance with the sections Sinai. measured by Goldberg (1963) at Makhtesh Hatira, The transgressive Daya Formation is Goldberg et al. (1971) at Gebel Maghara and by followed by the SHERIF FORMATION (Eliezri, in the author (herein) at Gebel El-Minshera. A Coates et al., 1963) and has a slight regressive generalized sketch of these sections is presented nature as indicated by a greater abundance of in Figures 7, 8 and 10. clastic material (clays and sandstones) than in the The Jurassic stratigraphy and paleogeography underlying Daya Formation and a northward shift of southern Israel was studied mainly by Goldberg of the occurrence of terrestrial elements (plant (1967, 1970) and Goldberg and Friedman (1974). remains, especially coal beds). The Sherif For an understanding of the stratigraphic Formation was divided in the subsurface into four descriptions and analysis presented herein, the members on the basis of prominent electric log characteristics of the Middle Jurassic markers (Fig. 2). As a whole, the Sherif lithostratigraphic i^nits in the Negev (southern Formation is made up of shale and some Israel; recognizable at Gebel Maghara in addition sandstone layers alternating with calcareous rocks to the formations recorded by Al-Far, 1966; Fig. in varying proportions; the lower part is sandy, 10) are briefly described (Fig. 2), based on the middle calcareous and the upper part, shaly. Goldberg and Friedman (1974). In its middle part, the Sherif Formation exposed The DAYA FORMATION (Eliezri, in Coates- at Gebel Maghara (Fig. 10) contains the Middle e t a l., 1963) consists mainly of carbonate with B athonian Micromphalites (subunits 57-61 of some shale and a few sandstone layers, Goldberg et al., 1971) overlain by the Upper transgressive over fluvial-deltaic sandstones of the Bathonian Bullatimorphites bullatus (d'Orbigny) (Fig. INMAR FORMATION (Nevo, 1963, modified by 3) and Eudesia species (in subunit 64). The Goldberg, 1964, 1970). The Daya Formation in Eudesia ranges up to top subunit 64 (Goldberg et the subsurface contains Bajocian microfossils a l., 1971). The Bathonian/Callovian boundary may (Maync, 1966) and was lithostratigraphically be tentatively placed some 40 m above the base correlated with the MAHMAL FORMATION (Nevo, of subunit 65, at the occurrence of the 1963, emended by Katz, 1968) exposed in foraminiferid Pseudocyclammina (?) smouti Banner, Makhtesh Ramon. Parnes (1981) established a which is known from Callovian-Early Oxfordian biostratigraphic correlation between the Mahmal rocks (Frenkel, 1975). However, 150 m above this Formation and the upper part of the Daya foraminiferid, at the middle of the overlying

c

Fig. 3. Bullatimorphites bullatus (d'Orbigny), (type 1442), x 1, M-7843, G. Maghara, Sherif Fm., subunit 64 (Goldberg et al., 1971), (Coll. F. Hirsch); U. Bathonian on basis of associated Eudesia species.

GSI Bull. 76, 1983 5 Z. LEWY U. CALLOVIAN AMMONITES

Zohar Formation (subunit 76), Frenkel (1975) Bogoch, 1978). distinguished the Meyendorffina bathonica Subzone The Brur Formation is overlain by the shaly which is regarded as Late Bathonian in age. KIDOD FORMATION (Rosenberg, in Coates et al., The Sherif Formation is overlain by the 1963) which overlies the Upper Zohar Formation ZOHAR^FORMATION (Rosenberg, in Coates et al., in the Negev, Israel. The Kidod shales above the 1963) which consists mainly of carbonate rocks Brur Formation may be coeval to both the Upper (108-182 m thick). In the Negev this formation Zohar and the Kidod formations, as well as to was divided on the basis of electric log markers the lower part of the Be'er Sheva Formation in into four members. The two lower members (the the Negev, although erosion of a lithostratigraphic Lower Member overlying the Hakana'im Member) equivalent of the Upper Zohar Formation in the form the Lower Zohar Formation, which is coastal plain cannot be excluded (Barzel and composed of thick calcarenite layers interbedded Friedman, 1970, p. 188) as indicated by the with thin layers of shale. The shale content varying thickness and the dolomitization of the tends to decrease toward the NW (seaward in Brur Formation. Moshkovitz and Ehrlich (1981) Jurassic time) forming a calcarenite unit in the recorded a biostratigraphic unconformity in the coastal plain of Israel (BRUR FORMATION, "Brur coastal plain of Israel between the Upper Calcarenite"; Derin and Reiss, 1966; p. 11, 13; Callovian-Oxfordian nannofossil Watznaueria Goldberg, 1970). The lithological change between manivltae Bukry in the Kidod Formation and the the Lower Zohar and the Upper Zohar Formation foraminiferid Meyendorffina bathonica Assemblage is marked by the electric log marker R (Goldberg, Zone in the Brur Formation below (attributed to 1970; herein Fig. 2). Near or at the top of the the Upper Bathonian). Lower Zohar Formation (or its lithostratigraphic *The»*Kidod“ Formation*4n Makhtesh Hatira equivalent: Brur Formation; Barzel and Friedman, contains Upper Callovian ammonites (Gill and 1970), Meyendorffina bathonica Aurouze and Tintant, 1975) whereas at Gebel Maghara Bizon occurs (e.g., in drillhole Zohar 5). The two (northern Sinai) and Mount Hermon it contains upper members, which form the Upper Zohar Creniceras renggeri (Oppel) of Early Oxfordian age Formation in the northern Negev (Halamish at its base. Member-and-overlying Tsia Member), consist of An increase in the carbonate content of the limestone with a varying shale content, locally shales, probably due to a lowering of the sea exceeding that of the carbonates. They are quite level and the development of normal benthic sim ilar to the lower two members with the communities (corals and molluscs) resulted in the general dominance of carbonate characterizing deposition of. the limy-marly .If&CRilSHEVA the Zohar Formation as a calcareous unit, and JFCrftMSTlON (Rosenberg in Coates et ah, 1963) thereby distinguish it from the shaly Kidod which locally interfingers and generally overlies Formation above and the rather shaly Sherif the Kidod Formation (Fig. 2). Formation below. Except for a single outcrop in the Samaria The^twowuppero^members of the . Zohar region (Wadi El-M alih; Fig. 1), the Jurassic Formation-show~.remarkable.-lateral lithofacies sequence in central and northern Israel was variations,.’as well as indications of local studied only from boreholes (unpublished internal unconformities in the eastern region. Sandy layers reports of oil companies). Due to remarkable and dolostones occur in the Halamish Member and lithofacies changes, some of the formations of in the lower part of the Tsia Member in the the Negev could not be distinguished in the northeastern Negev. Some of the dolostones are coastal plain of Israel. Therefore, several regarded as syngenetic (Gill, 1966) and are geographically limited formations were associated with mud-cracks in Makhtesh Hazera established, some whose precise correlation with (=Makhtesh Qatan), some of which may have those in the northern Negev is unknown. The most developed into erosion or tidal channels, indicating comprehensive studies of the Jurassic sequence in the subaerial exposure of this region (Gill, 1966; the subsurface of Israel were carried out by Goldberg, 1967). Maync (1966) and by Derin (1974) and Derin and TY\e Brur ? or matvou UltYvostratigraphvc Reiss (.19S6V equivalent of the Lower Zohar Formation) is made up o f 30-90 m detrital limestone, partly or completely dolomitized in some drilling samples in the coastal plain of Israel (Goldberg and

6 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

n. Chronostratigraphy

REVISED MIDDLE JURASSIC (a) Previous works STRATIGRAPHY OF THE MIDDLE EAST The Jurassic outcrop at Makhtesh Hatira was subdivided by Hudson (1958) into five biostratigraphic units, dating from Middle I. Ammonite Assemblages Callovian to Late Oxfordian with a probable Early The distribution pattern of the Jurassic Callovian age for the lowermost layers. The ammonites from southern Israel and northern Sinai Middle Callovian age of the lower part of the allows a distinction between two assemblages, exposure was based on the presence of defined by the exclusive occurrences o f very few Erymnoceras aff. dorotheae Spath (determined by taxa in each assemblage. L.F. Spath). Instead of relating to the age of 1) The Lower Assemblage exclusively contains the species dorotheae, which occurs in the Upper species of Levanticeras nov. gen. Callovian Athleta Zone in Cutch (Spath, 2) The Upper Assemblage exclusively contains 1927-1931, p. 220), and on the associated several members of the Oppeliidae (e.g., species of Pachyceras spp. (Hudson, 1958, p. 418), Hudson Brightia, Paeuddbrighitia, Kheraltes, Lunuloceras (1958) emphasized the genus Erymnoceras, which and Distichoceras) and probably also is a European Mid-Callovian index taxon. Due to exclusively Sowerbyceras tietzei (Till). the rather low chronostratigraphic significance of Both assemblages contain many common most invertebrate groups studied for the ammonites such as Pachyerymnoceras and recognition of substages (e.g., Mollusca: Reiner, Pachyceras species and cf. Lamberticeras henrici 1968; Hirsch, 1976, 1980; Nannofossils: Moshkovitz (R. DouvilM). and Ehrlich, 1976, 1981), Hudson's (1958) The Lower Assemblage is well represented at chronostratigraphy was used as the basis for all Makhtesh Hatira within the Tsia Member (Figs. 7, other stratigraphic studies in Israel (e.g., Maync, 9, 10) and at Gebel El-Minshera in units 3-6 1966). (Fig. 8). The Upper Assemblage is best G ill and Tintant (1975) published a short note represented at Gebel Maghara in the top of the on the Jurassic ammonite biostratigraphy of Upper Zohar Formation (upper 10 m of subunit 82 Makhtesh Hatira, dividing the lower 155 m of of Goldberg et al., 1971) and occurs in unit 7, the exposed 205 m into the Middle Callovian top Upper Zohar Formation at Gebel El-Minshera Coronatum Zone (from 10 m above base to 60 (Figs. 8, 9, 10). At these localities, the Upper m) and the Upper Callovian Athleta Zone (from Assemblage is overlain by the shaly Kidod 60 to 155 m). Although the so-called Mid-Callovian Formation, which contains Creniceras renggeri Erymnoceras philbyi of GiU and Tintant (1975) is (Oppel) of Early Oxfordian age at its base (in associated with Pachyceras lalandeanum (d'Orbigny) Gebel Maghara). The Upper Assemblage may be of Late Callovian age (e.g., Charpy and Thierry, recognized at Makhtesh Hatira by a few 1977), they (Gill and Tintant, 1975, p. 103) Oppeliidae in the lower part of the Be'er Sheva rejected the comment of Zeiss (1974, p. 273) that Formation (herein, and in Gill and Tintant, 1975). the Arabian Erymnoceras philbyi, as well as E. " Paraspidoceras" sp. and the Pachyceras and d oroth eae Spath from Cutch are actually Pachyerymnoceras are also present. A similar Pachyerymnoceras species. oppeliid-Paraspidoceras assemblage is recorded by Intensive microfaunal analyses were carried Gill and Tintant (1975), ranging up to 155 m out on subsurface samples from drillings in the above the base of the Tsia Member. Negev and the coastal plain of Israel in addition The argillaceous limestone in which the Upper to the studies on the large invertebrates from Assemblage occurs in northern Sinai differs the few outcrops. Meyendorffina bathonica Aurouze considerably from the reefal limestone below it, and Bizon (foraminiferid) at the top of the Lower which contains the Lower Assemblage at Gebel Zohar Formation (drillhole Zohar 5) dated this El-Minshera. At Gebel Maghara, this reefal level in the Negev as Late Bathonian. It is lithofacies may have been originally barren of overlain by the Upper Zohar Formation which ammonites or its hard nature may prevent their contains from its base upward the recognition in the rock; in any case, to date, the Callovian-Oxfordian nannofossil Stephanolithion Lower Assemblage has not been discerned at bigoti Deflandre (Moshkovitz and Ehrlich, 1976). Gebel Maghara. These stratigraphical relations in the Negev were

GSI Bull. 76, 1983 7 Z. LEWY U. CALLOVIAN AMMONITES

regarded conformable in the absence of short coronoides is regarded as a Mid-Callovian species, ranging fossils. In the coastal plain of Israel the Ldczy (1915, p. 452) recorded it from the Meyendorffina bathonica Assemblage Zone occurs Athleta Zone (his O ,) of western France, Swiss in the'upper part of the Brur Formation (=Lower Alps, southern Germany and Poland. Similarly Zohar; Barzel and Friedman, 1970). This formation Kinkelinicerds sp. cf. K. kinkelini (Dacqu^) is overlain by the shaly Kidod Formation which resembles the Upper Callovian form recorded by contains the Upper Callovian-Oxfordian nannofossil Collignon (1958, pi. 29, fig. 135) and not the Watznaueria mantvitae Bukry, suggesting a Middle Callovian type species. Another Upper biostratigraphic unconformity (Moshkovitz and C a llo v ia n Kinkeliniceras has been recently Ehrlich, 1981). described by Kanjilal and Singh (1980) supporting the extension of the range of this genus into the ( b ) R e v i s e d Middle J u r a s s i c a m m o n it e Upper Callovian. In both above mentioned chronostratigraphy examples the Israeli specimens are compared to Upper Callovian forms which Lrfczy (1915) and The ammonite assemblages from the three Collignon (1958) named as Middle Callovian species outcrops studied comprise Upper Callovian taxa although attributing them to the Upper Callovian. such as Pachyceras, Pachyerymnoceras Alligatlceras Therefore, the doubtful specific identification, as and Euaspidoceras, which date as Late Callovian well as the Mid-Callovian age, is insignificant and all the associated genera and species of the reference is made to a certain recorded questionable identity. No unequivocally exclusive specimen and its stratigraphic level. Lower or Middle Callovian species have been Both local ammonite assemblages contain found below the Upper Callovian forms. Similarly, Pachyceras and Pachyerymnoceras, which are no exclusively Oxfordian species occurs in the regarded as dimorphs (Pachyceras, the macroconch upper part of the Be'er Sheva Formation at o f Pachyerymnoceras; Callomon, 1963). Makhtesh Hatira, which was lithostratigraphically correlated with Oxfordian limestones in the Accordingly, they must be considered as coeval. Pachyceras appeared in Europe at the top of the subsurface (Negev; Goldberg, 1963). However, Athleta Zone (upper Spinosum Subzone of Brightia sp. A from the top of the Be'er Sheva Callomon and Sykes, in Duff, 1980) and became Formation at-Makhtesh Hatira, high above the abundant in the Lamberti Zone (Callomon, 1981, Upper Callovian ammonites at the base of this pers. comm.; Charpy and Thierry, 1977), formation, as well as above those recorded by characterized by Pach ycera s lalandeanum Gill and Tintant (1975), may already be of (d'Orbigny). Oxfordiarr*age. Such an age fo r the upper part of In Makhtesh Hatira and Gebel El-Minshera, the—Be'er Sheva Formation is-supported-by the Pachyceras appears above Pachyerymnoceras and occurrence of the Early Oxfordian foraminiferid becomes abundant in the Upper Assemblage. Gill Flabellocycloltna reissl Hottinger, 180 m above the and Tintant (1975) recorded new Pachyceratidae base of the Tsia Member (H. Frenkel, in Hirsch, together with P. lalandeanum at Makhtesh Hatira 1980, p. 159). Gill and Tintant (1975) recorded from the lower part of the sequence, from 30 m three-oppeliid species from the middle part of the above the base of the Tsia Member. This shortens Be'er- Sheva'Formation of this sequence, ranging the range of Pachyerymnoceras without Pachyceras up to 155 m above the base of the Tsia Member. to 20 m, which does not necessarily contradict They-are-associated^with Paraspldoceras which is the dimorphic relations of these taxa regarding found ’ lower bed together with the general scarcity of ammonites in the Pachyerymnoceras (Fig. 7) and may represent sequence. Late Callovian species. Therefore, the Callovian-Oxfordian boundary at Makhtesh Hatira is tentatively inserted (Fig. 7) above the last (c) Remarks on microfaunal chronostratigraphy occurrence of these oppeliids (35 m above the Some doubts as to the exclusive Late last occurrence of our Pachyerymnoceras) and Bathonian age of Meyendorffina bathonica Aurouze below the recorded Early Oxfordian foraminiferid. and Bizon (1958) have arisen during the present cf. Erymnoceras coronoides (Quenstedt) within survey of Gebel Maghara, northern Sinai. M. the Lower Assemblage of Makhtesh Hatira is a bathonica Subzone was distinguished there by poorly preserved fragment resembling the Frenkel (1975, p. 52) in the middle part of the Hungarian specimen of Loczy (1915). Although E. Zohar Formation (subunit 16 of Goldberg et al.,

8 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

1971). This level is situated approximately 220 m b u lla t u s and some 150 m above the above the ammonite Bullatimorphites bullatus Callovian-Lower Oxfordian foraminiferid (d'Orbigny) (Figs. 3 and 10) known in Europe from Pseudocyclammina(?) smouti Banner (Frenkel, 1975), the uppermost Bathonian and lowermost Callovian support the probable existence of M. bathonica beds (herein attributed to the Upper Bathonian during Callovian (at least Early) times (Fig. 10). due to its association with Eudesia, as well as to V ail et al., (1977) recorded a global its close position above the Middle Bathonian regression at the Bathonian-Callovian boundary Mtcromphalites; Fig. 10). The Callovian-Oxfordian followed by a quick Callovian transgression. M. foraminiferid Pseudocyclammina (?)smouti Banner bathonica occurs in Israel in the upper part of a (Frenkel, 1975) occurs 150 m below the M. reefal calcarenite (Lower Zohar Formation=Brur bathonica Subzone. If the M. bathonica Subzone Formation) overlying clay, oolitic limestone, marl was exclusively of Late Bathonian age, a sequence and silt (Karmon and Sederot formations=Sherif of some 200 m would have to be attributed to Formation; Fig. 11). This implies that M. the Upper Bathonian, whereas the Upper bathonica already lies high within the transgressive Callovian ammonites occur 100 m above this sequence, namely, in Callovian strata according to subzone (the base of the Upper Callovian is Vail et al. (1977). herein tentatively placed 20 m above M. bathonica Subzone at the base of the Upper Zohar (d) The boundary between the Lower and the Formation as suggested for the Negev, Israel). Upper Zohar Formation The foraminiferid M. bathonica was first described from the Paris Basin where it is found in The lower 9 m of the exposed Tsia Member a nodular limestone unit (Aurouze et al., 1956), at Makhtesh Hatira and the 25 m of the overlying Lower Bathonian rocks and overlain by Halamish Member below it (subsurface) did not oolitic limestone followed by dark colored marl of yield any ammonites (Fig. 7). The Late Callovian (Peltoceras athleta) age (Furrer Callovian-Oxfordian nannofossil Stephanolithion and Septfontaine, 1977). Therefore, the maximal bigott Deflandre occurs at the base of the range of M. bathonica could be from the Middle Halamish Member (base Upper Zohar Formation) Bathonian to the Middle Callovian. However, in the - (the range of S. bigoti, in the sense of Medd, Jura region (Dole, France) M. bathonica occurs in England is from the base of the Middle within the middle part of the Late Bathonian Callovian to the Lower Kimmeridgian; Medd, Clydontceras discus Range Zone. This is one of 1982). The Halamish Member overlies the top of very few stratigraphically controlled occurrences the Lower Zohar Formation which contains of this foraminiferid. According to Furrer and Meyendorffina bathonica (drillhole Zohar 5; Septfontaine (1977), M. bathonica may be missing Moshkovitz and Ehrlich, 1976). The 34 m barren in Upper Bathonian rocks containing Clydoniceras of ammonites at the base of the Upper Zohar discus of a certain lithofacies: Its absence in Formation in Makhtesh Hatira tire composed of similar rocks of Callovian age does not shale, clay, silt and sandy limestone and necessarily imply its non-existence during the dolostone layers (Goldberg, 1963). They show a Callovian. The stratigraphic control of M. gradual decrease in silt and sand from bottom to bathonica (and its accompanying Kilianina blancheti top and a transition from dolomite in the lower Pfender and Pfenderina sp.) is rather poor. This is part of Halamish Member to a sandy oolitic perhaps due to the lithofacies favored by these limestone at its top. The lower part of the foraminiferids, i.e., hard rock which is unsuitable overlying Tsia Member is sandy-marly becoming for the existence, preservation or recognition of limy upwards. Gill C1966) and Goldberg (1967) ammonites or other macrofossils. Thus all other described syngenetic dolomites and erosion levels in question were dated by a few channels in the lower part of the Tsia Member at occurrences of M. bathonica with Upper Makhtesh Hazera (20 km east of Makhtesh Bathonian fauna. Therefore, Furrer and Hatira), indicating that this region was shallow Septfontaine (1977) were careful in dating this marine and partly exposed at the time of so-called Upper Bathonian index fossil, giving it deposition. The lower part of the Upper Zohar a possible range of Middle-Upper Bathonian to Formation in the Negev’ apparently represents a Callovian(?). The occurrence of M. bathonica transgressive sequence with a high rate of Subzone at Gebel Maghara more than 200 m clastic deposition during a short period rather above the Upper Bathonian Bullatimorphites than a condensed sequence representing the time

GSI Bull. 76, 1983 9 Z. LEWY U. CALLOVIAN AMMONITES span between the Lower Callovian (post M. 1964a, 1964b, 1965), echinoids (Kier, 1972) and b a th on ica ) and the Upper Callovian. The other faunal groups recorded in Powers et al. clastic-enriched lower part of the Upper Zohar (1966) contributed additional stratigraphic data but Formation overlies fossiliferous calcarenite of the generally did not change the ages attributed by Lower Zohar Formation (Hakana'im Member), Arkell (1952) on the basis of the ammonites. forming a lithological break between the Lower Ammonites collected by a team of the U.S. and the Upper Zohar Formation. This boundary Geological Survey and ARAMCO geologists enabled c a n b e l i t h o s t r a t i g r a p h i e a l l y a n d Imlay (1970) to improve Arkell's (1952) ammonite biostratigraphically traced to the coastal plain of biostratigraphy of the same region. At the base Israel, where the Lower Zohar Formation of the of the Middle Dhruma Formation, Imlay (1970) Negev is regarded the lithostratigraphic equivalent distinguished a Spiroceras unit of Late Bajocian o f the Brur Formation (with Af. bathonica in its overlain by the Thambites and Dhrumaites unit of upper part). No limy lithostratigraphic equivalent Early Bathonian age, assigning Clydoniceras of the Upper Zohar Formation occurs there pseudodiscus Arkell to its upper part. The latter (Barzel and Friedman, 1970). The Brur Formation unit is overlain by the Tulites unit followed by varies in thickness (30-90 m) and shows local the Micromphalites and Thambites unit, both of dolomitization, mineralization and karstic Middle Bathonian age. The succeeding Dhrumaites phenomena (Goldberg and Bogoch, 1978; unit contains at its top D h r u m a ite s Buchbinder, 1979) (tinting at an unconformity cardioceratoides Arkell which Arkell (1952) with the Kidod Formation above, as indicated by attributed to the Upper Bathonian. Overlying this Foraminiferida and nannofossils (Moshkovitz and unit is the Upper Dhruma Formation which is Ehrlich, 1981). divided into two members: the lower limy 'Atash The boundary between the Lower and the Member (25 m) and the upper shaly Hisyan Upper Zohar Formation at Mount Hermon and Member (Fig. 10). The ’Atash Member is made Gebel Maghara is less clear. However, it is up of calcarenitic and some aphanitic limestone suggested that it be inserted at the top of the and contains the Bathonian brachiopods: Eudesia M eyendorffina bathonica Zone, at the top of ccrdtum (Lam.) and E. cardioides Douville' (Arkell, subunit 3 of the section at Majdal Shams (Mount 1952, p. 247; Powers et dt., 1966, PL 7). At 11 Hermon; Goldberg, 1969) where dolomitization, m above its base a new echinoid assemblage silicification and karst phenomena are abundant. occurs, comprising species different from those in At Gebel Maghara this boundary is placed herein the Middle Dhruma Formation (Kier, 1972). at top subunit 77 of Goldberg et al. (1971) Pachyceras cf. P. schloenbachi (Roman) and where silicification is common (M . bathonica Grossouvria sp. also first occur at the same level, Subzone recognized at siibunit 76); this unit is whereas several Pachyerymnoceras species start to overlain by shales with limonite concretions. appear (a little higher) below the top of this The boundary between the Lower and the member. This Pachyerymnoceras assemblage (Fig. Upper Zohar Formation is herein regarded as 10) ranges throughout the upper part of the indicating a profound paraconformity between the 'Atash Member into the Hisyan Member and the Upper Bathonian (Lower Callovian, as suggested in lower 25-40 m of the lower part of the Tuwaiq this study) Lower Zohar Formation (=Brur Mountain Formation (Imlay, 1970, p. D7). This Formation) and the Upper Callovian Upper Zohar assemblage comprises Pachyerymnoceras and Formation (probably correlative to the lower part Pachyceras species of Late Callovian age which of the Kidod Formation of the coastal plain of Israel (Fig. 11). were previously attributed by Arkell (1952) and Imlay (1970) to the Middle Callovian, and later in part redefined and redated by Zeiss (1974). The HI. Stratigraphic Correlation With Adjacent Regions Bathonian Eudesia species recorded by Arkell (1952, p. 247) from the 'Atash Member must have (a) Saudi Arabia originated from the lower 11 m, i.e., below the The biostratigraphy and the ages attributed beginning of the Upper Callovian ammonite to the lithological units of the Jurassic outcrops assemblage. Thus a paraconformity is inserted at at Gebel Tuwaiq (central Saudi Arabia) were based 11 m above base 'Atash Member, separating Upper mainly on ammonites (Arkell, 1952; Imlay, 1970). Bathonian rocks (with Eudesia) from Upper Other studies, such as on foraminiferids (Redmond; Callovian rocks (Figs. 10, 11). From Arkell's (1952)

10 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY assumption that Dhrumaites does not range into overlying clay (containing the Lower Oxfordian the Lower Callovian, Imlay (1970, p. D7) noted Creniceras renggeri (Oppel); Haas, 1955) into the the absence of Early Callovian ammonites. Kier unit J5. Due to the remarkable lithological and (1972) suspected such an unconformity on the faunal change between the clay and the underlying basis of the complete change in the echinoid argillaceous limestone, several authors considered assemblages between the Middle and Upper (11 m the J5 as comprising only the Lower Oxfordian above base 'Atash Member) Dhruma Formation. clays, known in Israel as the Kidod Formation. Dunnington et al. (1959) indicated a similar The Meyendorffina bathonica Zone in this section Bathonian-Callovian unconformity in Iraq. was traced by Derin (in Goldberg, 1969) throughout a biomicritic limestone (subunits 1-3 of (b) Lebanon and Syria Goldberg, 1969) at the upper part of which The most studied Jurassic outcrops of karstic phenomena and dolomite with chert nodules Lebanon and Syria occur at Mount Hermon. The occur, suggesting a sedimentary omission surface. Jurassic strata at its southern flank were This surface is herein regarded as the boundary measured and sampled by Goldberg (1969), who between the Lower and the Upper Zohar assigned Israeli formation names to the lithologic Formation where the boundary between the units J1-J7 described by Dubertret (e.g., 1963, Bathonian (or Lower Callovian) and the Upper 1966). Ponikarov (1967) made a synthesis of Callovian is tentatively inserted. litho-, bio- and chronostratigraphic units dividing the sequence into J 1-3 with subdivisions (c) Abu Darag Region, Eastern Egypt according to stages (e.g., J2bt = Bathonian; J3cl The ammonites of the Jurassic outcrops in = Callovian). The 717 m of the Callovian J3cl the Abu Darag region (western side of Gulf of consists of 700 m of limestone attributed to Suez) recorded by Abdallah et al., (1965) seem to both the Lower and Upper Callovian which contain belong to the Upper Callovian on the basis of Erymnoceras at^the' top. The remaining overlying Pach ycera s c f. lalandei and the so-called 17 m consists of argillaceous limestone containing Erymnoceras and Clydoniceras, recalling the Upper Callovian ammonites (Ponikarov, 1967). Pachyerymnoceras and Levanticeras nov. gen. of Dubertret (1955, 1966) recorded Erymnoceras northern Sinai. Nubidites omarai of Wiedmann and coronatum (Bruguifere) from this upper unit (14.5 Kullmann (1979) from Nubian sandstone near Abu m) and attributed it to the Upper Callovian on Darag is herein suspected to be a young the basis of accompanying Upper Callovian Levanticeras levantlnense nov. gen. and sp., and ammonite species. This casts some doubt on the probably the Clydoniceras of Abdallah et al. identification of E. coronatum which is herein (1965). However, due to its very young stage it suspected to be a Pachyerymnoceras species. is difficult to compare it to our advanced growth ?Quenstedtoceras (Pavloviceras) ?mariae stages. The—Jurassic outcrop at Abu Darag is (d'Orbigny) from Mount Hermon (Haas, 1955, p. herein regarded as representing the Late 120, PI. 18, Figs. 22-25) is quite a large, limy, Callovian transgression (Athleta-Lamberti Zone) as natural cast from an unknown precise in northern Sinai and Israel. stratigraphic level within the Callovian-Oxfordian fossiliferous sequence. It differs by its dimensions (d) Zerqa River, Jordan and limy nature from the pyritized, rather small ammonites of Early Oxfordian age described by A few outcrops of Jurassic sediments occur Haas (1955) from this locality. This single, in the central Jordan Valley along a segment of corroded ammonite closely resembles the the Zerqa River (Yaboq). Most fossils collected Pachyceras-like adult stage of Pachyerymnoceras there point to Bajocian (?) and Bathonian ages (Late Callovian). Due to its calcareous composition whereas some paleontologists extended their ages to it * is thought to originate from the fossiliferous the Callovian and even to the Oxfordian (see in argillaceous limestone (top Zohar Formation) just Bender, 1974; Basha, 1980); The lithostratigraphic below the dark shale with the pyritized fauna correlation of the Jurassic strata in the Zerqa (Kidod Formation), from which Upper Callovian River area with those in Israel as suggested by ammonites were recorded (Dubertret, 1955, Bandel (1981) lacks the necessary biostratigraphic 1963; Ponikarov, 1967). and chronostratigraphic data for the recognition of Dubertret (1963) combined the 14.5 m of the the equivalents to the Upper Callovian Zohar and fossiliferous argillaceous limestone with the Kidod formations of Makhtesh Hatira in Jordan

GSI Bull. 76, 1983 11 Z. LEWY U. CALLOVIAN AMMONITES

(Bandel, 1981, p. 290). The occurrence of Eudesia of earlier strata, seems to be well dated (Late near the top of this sequence indicates a Middle Callovian) and isochronous. The similar ammonite to Late Bathonian age for the upper part of the assemblages in the lower part of the Late Jurassic sequence at the Zerqa River area Callovian transgression suggest that it was (Delance, 1982, pers. comm.). extensive and rapid. Therefore, the 34 m of mainly clastic sediments (Halamish Member and lower 9 m of the Tsia Member) barren of ammonites, at the base of this transgressive THE NATURE OF THE UNCONFORMITY sequence at Makhtesh Hatira (Negev, Israel) are The local karstic phenomena, dolomitization assumed to represent a high rate of sedimentation and mineralization of the Brur Formation (= and unfavorable living conditions for ammonites Lower Zohar Formation) in the coastal plain of (although the lack of ammonites even in the Israel (e.g., Buchbinder, 1979), associated with a exposed basal 9 m of the Tsia Member at biostratigraphic unconformity (Moshkovitz and Makhtesh Hatira may be due to their general Ehrlich, 1981) is the only clear evidence of an scarcity, as well as to the small dimensions of unconformity there between Upper Bathonian (or the exposure). Since this lower part of the Upper Lower Callovian, as suggested herein) and Upper Zohar Formation is herein regarded as a rapidly Callovian (?Lower Oxfordian) rocks. This deposited, mainly clastic (sea-marginal to shallow unconformity is traced throughout Israel and marine) unit at the beginning of the transgression, northern Sinai to central Saudi Arabia. The it is dated as Late Callovian on the basis of lithologv on both sides of the assumed similarly dated ammonites or nannofossils at the unconformity plane is quite similar and no base of the transgressive sequence in Saudi Arabia change in the bedding plane, no conglomerates or and the coastal plain of Israel. undisputed hardgrounds occur. However, a The following environmental development reevaluation of the minor lithological changes at during the late Mid-Jurassic is suggested to have this level makes it possible to reconsider the formed the proposed paraconformity with a hiatus presence of a paraconformity between the Lower of up to 4-5 million years in Saudi Arabia and the Upper Zohar Formation, for example at (according to van Hinte's, 1976, time scale). During Makhtesh Hatira, which was noted by Goldberg the Late Bathonian, the present-day regions of (1963). He later ignored this paraconformity due northern Sinai, Israel, Lebanon and central Saudi to the excellent lithostratigraphic correlation of Arabia were part of an almost level, shallow the formations and members of the Mid-Jurassic marine shelf environment. The level nature of sequence across the Negev (Israel) to northern the bottom was attained following a long period of Sinai, which more or less retain the same nature clastic supply from the continent, which and thickness (e.g., Goldberg and Friedman, 1974). gradually also levelled the nearby terrestrial The hiatus at Gebel Tuwaiq ranges from the regions. This terrigenous material intermixed with latest Bathonian to the Late Callovian. The extent the marine carbonate particles, mainly skeletons of this hiatus in Israel and Sinai is less clear and of benthonic organisms, all well-distributed by the would be considerably reduced if M. bathonica currents (demonstrated by the clear and extensive really did range into the Early Callovian and even lithostratigraphic correlation of the members of more so if it ranged into the Middle Callovian. the Sherif Formation). In Early Callovian (as Nevertheless, the clear biostratigraphic suggested herein) times, a minor transgression unconformity at Gebel Tuwaiq and in the coastal resulted in the accumulation of reefal limestone. plain of Israel suggests a similar situation in the Thereafter, this shallow marine area was exposed Negev (Israel). without discernible tilting. This drop in sea level Late Callovian ammonites (Pachyerymnoceras, was possibly caused by a regional eustatic event as well as Pachyceras or Levanticeras nov. gen.) as a result of which the Tethys of the Middle are the first marine fossils in the lowermost East retreated more than 100 km seawards. The part of the transgressive sequence, just above the level nature of the exposed shelf bottom and the Upper Bathonian (Gebel Tuwaiq) or Bathonian(?) nearby continent was not affected by the (coastal plain of Israel, Gebel Maghara) regression, hence resulting in a geographically assemblages, and at the base of the marine limited, very minor erosion of the exposed area. sequence at Abu Darag (Egypt). The beginning of Furthermore, during the gradual sea-level drop this transgression, which overlies different levels the unlithified rocks may have been subjected to

12 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY lagoonal and sabha-type environments, leading to part of a broad shelf surrounding the dolomitization and silicification and thus to Arabo-Nubian craton in Middle Jurassic times. hardening of the upper part of the exposed layers, Sea-level oscillations, as well as varying rates of which later resisted destruction by weathering supply of clastic material from the continent, (e.g., top Meyerdorffina bathonica Zone, subunit 3 were the main factors which determined the of Goldberg, 1969, at Mount Hermon; middle nature of the Middle Jurassic rocks (see: Zohar Formation, subunit 77 of Goldberg et al., Goldberg and Friedman, 1974). 1971, at Gebel Maghara, northern Sinai). The rather dry tropical conditions during the Tectonic quiescence during the time of Lower Liassic (evaporites of the Ardon Formation exposure prevented the development of relief and in southern Israel) were followed by a humid the accumulation of terrestrial clastic sediments tropical climate from Mid-Liassic times onward. in the lows. Only in limited regions (e.g., the This is indicated by the accumulation of thick southern coastal plain of Israel) were the exposed fluviatile and deltaic clastic sediments partly rocks subjected to some erosion and karstic intermixing with shallow marine ones, all rich in processes, leading to variations in thickness of iron-oxides and plant remains (Inmar Formation in the Brur Formation ( 30-90 m), dolomitization and Israel, Marrat Formation in Saudi Arabia), the mineralization of voids and channels by quartz resulting from a high rate of clastic supply from - fluorite- Fe-dolomite (Buchbinder, 1979) and the continent. A late Mid-Bajocian transgression siderite (L. Buchbinder, 1981, pers. comm.). penetrated landward and reached Makhtesh Ramon The upper part of the Lower Zohar in southern Israel (Daya Formation = Mahmal Formation (Hakanaiim Member), as well as its Formation). The marine environments during the lithostratigraphic equivalent in the coastal plain of Middle and Upper Bajocian are well represented Israel (Brur Formation), is generally composed of by fossiliferous marl and limestone in northern limestone. The overlying lower part of the Upper Sinai (Bir Maghara Formation = Daya Formation) Zohar Formation (Halamish Member) has a and Saudi Arabia (Lower Dhruma Formation). variable lithology in different regions (clay, marl, This Bajocian transgression is followed by a slight limestone and dolomite, all with varying amounts regression at the beginning of the Bathonian, of silt), changing upward into a "deeper marine" which deposited sandstone and shale with plant lithofacies. This transgressive nature characterizes remains in northern Sinai (lower part of Safa both members of the Upper Zohar Formation, with Formation of A l-F ar, 1966, lithostratigraphic a gradual increase in marine influence from the equivalent of the Sherif Formation in Israel). The lower Halamish Member into the overlying Tsia marine influence increased during the Middle and Member. Therefore, both are herein attributed to Upper Bathonian although generally, the whole the same sedimentary phase, which is assumed to region was under a very shallow sea and even have been rapid and of Late Callovian age, temporarily affected by terrestrial conditions although the first age-indicative ammonites occur (Mid-Bathonian coal bed at Gebel Maghara). The 9 m above base Tsia Member (Makhtesh Hatira, Middle and Upper Bathonian sediments were Negev, Israel; Fig. 7). Higher in the sequence, enriched in fine clastics forming shale layers the Upper Zohar Formation becomes limy, forming interbedded with limestones in northern Sinai, in together with the limy Lower Zohar Formation, a the northern Negev (Israel) and in the coastal calcareous unit clearly distinguished from the plain of Israel (Karmon Formation; Fig. 11). The shaly Sherif Formation below (or Karmon Bathonian-Callovian boundary may lie within this Formation; Fig. 11) and the Kidod Formation shaly lithofacies as proposed herein. Towards the above. upper part of this shaly unit, sandstone beds, A similar intraformational unconformity iron-oxide concretions, oncolites and gypsum occurs in central Saudi Arabia, where the occur and macrofossils become rare. This clastic discontinuity plane separates the 'Atash Member sequence indicates a period of great influx of (Upper Dhruma Formation) into a lower Late terrigenous material from the continent into the Bathonian sequence of 11 m, overlain by 14 m of broad, shallow marine environment, leading to a aphanitic limestone of Late Callovian age. leveling of the sea bottom, as well as of the nearby continent* accompanied by sea shallowing. GEOLOGICAL HISTORY Thereafter a rather rapid subsidence of the shelf The Middle Eastern countries (Egypt, Israel, region (approximately 20-40 m) occurred, resulting Jordan, Saudi Arabia, Lebanon and Syria) were in the sedimentation of aphanitic and calcarenitic

GSI Bull. 76, 1983 13 Z. LEWY U. CALLOVIAN AMMONITES

limestone containing corals, stromatoporoids with With the beginning of the Lower Oxfordian, some molluscs and brachiopods in northern Sinai the region seems to have subsided during another and the coastal plain of Israel (Brur Formation = eustatic (?) pulse, shifting the belt of benthic Lower Zohar Formation). This limy lithofacies productivity southeastward (landward). Bioclastic contains the Meyendorffina bathonica Assemblage carbonate supply into the newly formed "deep" mainly in its upper part, herein assumed to range marine regions was drastically reduced, whereas into the Lower Callovian. fine clastics accumulated, forming a thick shale unit (Kidod Formation, which started to In Early Callovian times (post Meyendorffina accumulate elsewhere already from the Upper bathonica Assemblage Zone), a regional eustatic Callovian; 155 m at Mount Hermon, J5; 64 m at drop in sea level occurred. Due to the rather Gebel Maghara). These shales contain very few level relief of the former broad, shallow benthonic faunas, mainly small, mud-dwelling shelf-region, this regression exposed large areas of bivalves (e.g., N ucula) whereas plankton the present-day Middle East. The gradually (foraminiferids and nannofossils e.g., Moshkovitz exposed level topography was subjected to minor and Ehrlich, 1976) and nekton (ammonites; e.g., erosion or non-deposition due to a lack of Haas, 1955) are abundant in the lower part of tectonism during this period. However, meteoric the shaly unit. All originally aragonitic skeletons water may have affected the exposed rocks formed pyritic internal moulds before dissolving. (karstic phenomena; Buchbinder, 1979). The lacuna The biota and the diagenetic processes indicate increases landwards up to an interval from the that the surface water was normal marine Late Bathonian to the Late Callovian at Gebel whereas at the bottom, reducing conditions Tuwaiq, Saudi Arabia. prevailed, perhaps due to oxygen consumption by The Late Callovian (Athleta-Lamberti Zone) the decomposition of the organic matter within sediments represent a rapid transgression in the the shales. The high rate of deposition resulted southern Tethyan regions, distributing European in the rapid burial of the undamaged skeletons in fauna into the Eritrean-Indian region (e.g., a non-bioturbated sediment. The rather small Pachyceras and Pachyerymnoceras in Eritrea, dimensions of the fauna (as well as the Somalia and Cutch). fine-grained sediments) point to a low energy environment, apparently with minor vertical The accumulation of residual clay minerals intermixing (during the same times, a similar which were earried seawards during the Late facies prevailed in Europe, known in England as Callovian transgression may have resulted from the Oxford Clay; e.g., Duff, 1975). Upwards in the pre-Upper Callovian aereal exposure and the shaly section fossils decrease in number and minor erosion. These fine clastics were distributed the environmental conditions seem to be by currents, forming a shaly unit (Kidod unfavorable even for nekton and plankton. This Formation) overlying the Brur Formation, whereas may be due to the closure of the area by a in the shallow marine environments these clays barrier reef (Nir'am Formation) which developed intermixed with the calcareous bioclastics more or less along the present-day Mediterranean forming the marl and argillaceous limestone of coastline of southern Israel, partly sealing the the Upper Zohar Formation in the Negev, Israel eastern (landward) basin from the open sea. (Fig. 11). Although the entire region (present-day This paleoenvironmental reconstruction Sinai, Lebanon, central Saudi Arabia) was a generally agrees with that suggested by Derin and shallow shelf, various sedimentary environments Gerry (1972, Fig. 4a), which differs from the prevailed due to the position of river-mouths, present scheme in the timing and in the current pattern and bathymetry. These factors pre-Upper Callovian lacuna. However, both controlled the development of coral reefs and schemes suffer from lack of precise age other faunal niches, as well as the dispersal of determination of the Kidod Formation, overlying fine clastics and the formation of dolomite in the Brur Formation in the coastal plain of Israel lagoons. Thus from the Late Callovian onward, (suggested here to be of Late Callovian age, limestone and marl (Upper Zohar and lower part coeval to the Upper Zohar Formation - see: o f Be'er-Sheva Formation) or pure limestone Barzel and Friedman, 1970) which bears directly (partly dolomitized; Nir'am Formation) on the geological history of the area. accumulated, interfingering and intermixing with clays (Kidod Formation).

14 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

SYSTEMATIC PALEONTOLOGY form of Haas (1955, PI. 1, figs. 6-7) is excluded herein from the synonymy. The main saddles in The systematic order of the descriptions of the suture of P. plicatum are diphylloid, so that the ammonites is based on Arkell (1957) with this species should have been assigned to some emendations according to Donovan et al. Hypophylloceras rather than to Phylloceras s. str. (1981). The small number of specimens, as well according to the criteria suggested by Wiedmann as their state of preservation precluded relating (1962). However, Hypophylloceras is attributed to them to the suggested dimorphic connections the Cretaceous only, therefore, for the time between Pachyceras and Pachyerymnoceras or being the species plicatum is still included in between Peltoceras and Rursiceras (e.g., Charpy Phylloceras. and Thierry, 1977; Callomon, 1963; Callomon, pers. comm., 1981). Hence these taxa are herein AGE: Ldczy (1915, p. 450) recorded P. plicatum described as separate genera. from the Lower Bathonian to Upper Oxfordian The morphological features measured are strata in south-central Europe. The specimens of diameter (D), height of whorl (H), its width (W) Noetling (1887) and Haas (1955) originate from and the diameter *of the umbilicus (U); all Lower Oxfordian shales (Kidod Formation; measurements are in millimeters. Renggeri-Zone) at Mount Hermon, whereas our A ll illustrations are in natural size unless specimens occur in the underlying Zohar otherwise marked. Arrows indicate the last septal Formation. suture and the beginning of the body-chamber. MATERIAL AND OCCURRENCE: (Type No. 1231) M-6046, 5384 (coll. M. Goldberg and M. Raab), Makhtesh Hatira, Upper Zohar Formation (Tsia Member); M-7745(6) (coll. Z. Lewy), Gebel Family PHYLLOCERATIDAE Zittel, 1884 Maghara, top Zohar Formation; M-7852 (coll. Z. Genus and Subgenus PHYLLOCERAS Suess, 1865 Lewy), Gebel El-Minshera, top Zohar Formation (Unit 7). Type species: Am. heterophyllus J. Sowerby, 1820

Phylloceras (Phylloceras) plicatum Neumayr Genus SOWERBYCERAS Parona and Bonarelli, PI. 1, fig. 5 1895 1887 Phylloceras plicatum Neumayr, Noetling, p. Type species: Ammonites tortisulcatus d'Orbigny, 14; PL 2, fig. 2. 1915 Phylloceras plicatum Neumayr, Loczy, p. 1849 283; text-fig. 6. Sowerbyceras tietzei Till 1955 Phylloceras (Phylloceras) plicatum Neumayr, PI. 1, figs. 1-3 Haas, p. 14; PL 1, figs. 1-5, 8-13. 1915 Phylloceras tietzei Till, Loczy, p. 305; PI. DESCRIPTION: Involutely coiled, whorl section 3, figs. 2-3, text-figs. 28-29. compressed, ovate with subparallel flanks in the inner whorls, becoming with growth more rounded and inflated in the middle of the flanks. W/H increases with growth from 12.1/20.6 = 0.59 to DESCRIPTION: Involutely coiled, compressed 29/44 = 0.66. The shell is ornamented by fine, conch with flattened flanks and an almost flat flexuous striae, superimposed on very low, venter. The. umbilicus is small with a low similarly flexuous lateral ribs. Each stria may be rounded wall. The dimensions of the best traced from the umbilical seam across the preserved specimen (M-7745) are: D = 36.0, H = venter without furcating. Therefore, the striae are 18.3(0.50), W = 14.3(0.40), W/H = 0.78, U = very fine and dense near the umbilicus, becoming 5.6(0.16). The internal mould is smooth, with relatively broader and more widely spaced strongly prorsiradiate constrictions, five per towards the venter which they cross with a gentle volution (D = 36 mm) which vary in strength but adorally convex flexure. Sutures not preserved. keep the ventral rib-like pre-constrictional labial DISCUSSION: The compressed, ovate whorl ridges in all specimens (PI. 1, fig. 3). The section and the striae superimposed on low ribs constrictions are sygmoidal with a strong labial, characterize this species. Therefore, the broad adapical curvature. Sutures not preseved.

15 GSI Bull. 76, 1983 Z. LEWY U. CALLOVIAN AMMONITES

DISCUSSION: The strongly prorsiradiate Family LYTOCERATIDAE Neumayr, 1875 constrictions and the whorl section are similar Genus LYTOCERAS Suess, 1865 tothose of Sowerbyceras tietzei Till of L

16 GSl Bi ll. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

DESCRIPTION: A small (D = 26 mm) half Kheraites ferrugineus Spath specimen, slightly corroded, rather involutely PI. I, figs. 9-12 coiled (U/D approximately 0.29); whorl section 1928 Kheraites ferrugineus Spath, p. 110; PI. 9, high and narrow (W/H = 7/13 = 0.54) with a figs. 6 a-c. fastigate, unicarinate venter, subparallel flanks, 1951 Kheraites ferrugineus Spath, Jeannet, p. 51; angular, umbilical shoulder and a steep, low PI. 11, figs. 5-7, text-figs. 111-112. umbilical wall. The shell is ornamented by low, gently DESCRIPTION: Evolutely coiled, planulate conch. falcoid ribs which are very weak or even absent The whorl section is almost quadrangular with at the dorsal part of the flanks, strengthening sub-parallel flanks and a broad, low ventrally although remaining low. Some ribs fastigate venter. bifurcate at the middle of the flank, thereby, MEASUREMENTS: changing slightly from prorsiradiate to radiate. The venter and the umbilical wall are smooth. D H W. max. W/H U

Sutures not preserved. M- 7 7 4 5 :1 30.5 14.6(0.48) 11 . 3 (0.37) 0.77 8.3 (0.27)

DISCUSSION: Our specimen is very similar to M-7 7 4 5 :1 41 .5 19. 3 (0.46) 14.0(0.33) 0.7Z 11.2(0.27) the other recorded lurvuloides specimens but its poor state of preservation does not enable undoubtable specific identification. Among the The young ontogenetic stage is smooth up to a specimens attributed by Jeannet (1951) to diameter of 6-7 mm, where ribs appear, becoming lunuloides are some quite evolute (U/D = 0.37) stronger with growth. Over a diameter of 15 and broad (W/H = 0.63) ones which mm, it attains the characteristic ornament of stratigraphically occur above the typical forms. falcoid primary ribs, some of which bifurcate at Lunuloceras cf. grossouvrei Par. and Bon. in the middle of the flanks. The primaries are Jeannet (1951, p. 59; PI. 13, figs. 7-8) are rather intercalated by short ventrolateral secondaries involute and compressed with weak to almost no which may approach the primaries looking as if ornament on the dorsal half of the flanks. Thus they furcate from them. All ribs become broader our specimen, like that of Corroy (1932), is close and stronger on the venter in the form of to some of the .morphological varieties included prorsiradiate bullae, joining the more elevated by Jeannet under lunuloides and cf. grossouvrei. siphonal keel. The keel is slightly crenulate with Orbignyceras paulowi Tsytovitch of Jeannet (1951) lows in-between consequent ventral ribs. The comprises a variety of morphotypes, ranging from dorsolateral parts of the primary ribs appear as Middle Callovian to the Lower Oxfordian. Some bullae due to some weakening and thinning of the of these specimens resemble our fragment, ribs at the middle of the flanks of the young although most have well developed concave stage. Sutures not preserved. ventral shoulders, forming a biconcave venter. Gill DISCUSSION: Our specimens closely resemble and Tintant (1975) recorded (without figuring) those from Cutch and Switzerland, although our Sublunuloceras discoides Spath, from the same single complete specimen has a smaller umbilicus stratigraphic level in Makhtesh Hatira where our and narrower whorl sections. specimen originates; therefore, it is possible that it represents the same form. AGE: Spath's (1928) type material originates from AGE: Jeannet (1951, p. 58) recorded this species the Middle Callovian of Cutch. The Swiss specimen of Jeannet (1951, p. 51) is attributed from lowermost Callovian, Middle Callovian to to the uppermost Callovian (Lamberti-Zone). Lower Oxfordian rocks. MATERIAL AND OCCURRENCE: (Type No. 1381) MATERIAL AND OCCURRENCE: (Type No. 1366) M-7745(6) (coll. Z. Lewy), Gebel Maghara, top 1^7810 (coll. F. Hirsch), Makhtesh Hatira, lower Zohar Formation. part of Be'er Sheva Formation.

Kheraites intermedium (Spath) genus KHERAITES Spath, 1925 PI. 1, figs. 15, 16

Type species: Harpoceras crassefalcatum Waagen, 1928 Putealiceras intermedium Spath, p. 112; PI. 1875 11, figs. 9a, b.

GSI Bull. 76, 1983 17 Z. LEWY U. CALLOVIAN AMMONITES

1928 Putealiceras intermedium samatrense Spath, advanced growth stage of P. intermedium p. 112; PI. 14, fig. 4. irregularis Collignon tends to approach the shape cf. 1951 Rossiensiceras cf. rossiense Teisseyre, of the unicarinate intermedium Spath. Jeannet, p. 49; PI. 11, figs. 1-2 (not 3), text-figs. AGE: K. intermedium occurs in Cutch together 106 b,c, 107a. with Pachyceras indicum Spath in uppermost ? 1975 Putealiceras intermedium Spath, Gill and Callovian rocks (Duncani to Lamberti Zones; Tintant, p. 108. Spath, 1928, p. 113).

DESCRIPTION: Evolutely, coiled, planulate, MATERIAL AND OCCURRENCE: (Type No. 1382) compressed conchs. Whorl section high (W/H = M-7745(ll) coll. Z. Lewy), Gebel Maghara, top 0.62), trapezoidal with a fastigate unicarinate Zohar Formation. venter. The ornament consists of falcoid primary ribs with a shorter secondary one in between each pair of primaries, starting near the middle of Genus BRIGHTIA Rollier, 1922 the flank as if the primaries bifurcate. The umbilicolateral part of the ribs tends to weaken Type species: Hecticoceras nodosum Bonarelli, and disappear in advanced growth stages whereas 1893 the ventrolateral part becomes broader and lower, REMARKS: Most authors attribute to species of form ing the ventrolateral shoulder. Generally, Brightia a broad range of intraspecific ornament weakens with growth (PI. 1, fig. 16). morphological variations, some of which resemble The venter is smooth, fastigate and unicarinate other species. To reach an undoubtable throughout ontogeny. identification, several well-preserved specimens are needed. Due to the fragmentary, corroded state DISCUSSION: This species has a more compressed of our material, the specific identifications are whorl section, lower and less fluxuous ribbing and very tentative. a higher fastigate venter than K. ferrugineus. It is Herein attributed to Kheraites rather than Putealiceras due to its unicarinate venter and Brightia sp. A quite coarse ribbing in early ontogenetic stages. PI. 1, figs. 17, 18 Some of the specimens attributed by Jeannet (1951) to Rossiensiceras cf. rossiense resemble K. DESCRIPTION: Small (D = 34.5 mm), broken and intermedium in whorl section and ornament, partly corroded specimens. especially those with the widely-spaced ribbing MEASUREMENTS: from the Late Callovian. Gill and Tintant (1975) recorded Putealiceras intermedium from the lower part o f the Be'er Sheva Formation of Makhtesh M-7670 D H W W/H U

Hatira (Israel), the herein assumed biostratigraphic 34.5 14.1(0.40) 9.7(0.27) 0.68 12(0.35) equivalent of top Zohar Formation of Gebel Maghara. P. intermedium samatrense Spath (1928, PI. 14, fig. 4) is identical in ribbing, whorl section and weakening of ornament in advanced Strong prorsidradiate, bullate, dorsolateral ribs growth stages to our specimens, all being similar bifurcate at the dorsal third of the flank. They to the typical intermedium (Spath, 1928, PI. 11, continue for a short distance as very low figs. 9a,b) in mode of ornament and whorl prorsiradiate ribs, which turn back strongly at section. The coarsely ornamented subspecies the dorsal 2/5 of the flank, forming an angle of intermedium robusta Spath (1928, PI. 12, figs. approx. 125 . The ribs weaken near the fastigate 9a,b) has a quite similar whorl section, but and smooth venter. At the angular turning-point differs by its very coarse ribbing even in of the ribs, they may be low so that it seems as advanced growth stages and therefore it is not if a furrow occurs between the dorsolateral, included herein in the synonymy. Putealiceras strong bullae and the ventrolateral ribs (PI. 1, intermedium and P. intermedium irregularis of fig. 17). The bullae and the ribs are as broad as Collignon (1958; PI. 33, figs. 158, 159) have a their interspaces, thus forming a similar pattern broad whorl section with a broad, low venter, in the dorsal and ventral regions of the flanks. especially in the young stage, whereas the Sutures not preserved.

18 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

DISCUSSION: The whorl section, the fastigate, 1951 Brightia metomphala Bonarelli, Jeannet, p. unicarinate venter and the ornament are of 64; PL 14, figs. 2-4, text-figs. 143-145. Brightia. Our specimen is an internal mould and 1961 Hecticoceras metomphalum Bonarelli, has broad, low, rather widely-spaced ribs which Rangheard, p. 154; PI. 3, figs. 6-7, occur in some Putealiceras and Campylites species text-fig. 9. (e.g.f P’ schummachert (Noetling) in Haas, 1955; 1975 Putealiceras (Putealiceras) metomphalum PL 9, figs. 38-40). The venter of our specimen (Bonarelli), Lominadze, p. 34; PI. 1, figs. 5-7; PI. 2, neither has ventrolateral keels in addition to the figs. 1-5; text-fig. 6. siphonal one, nor faint ribs, so that a relation 1975 putealiceras (Putealiceras) metomphalum to species o f the above mentioned genera is mJtiooStatum Cfcytovitch), Lominadze, p. 37; PL 2, excluded. Some Brightia species in Jeannet (1951) figs. 6-7. and Lominadze (1975) have a broad range of DESCRIPTION: Evolutely coiled, compressed morphological variations in respect to ribbing conchs. Whorl section high (W/H = 0.67, 0.76), density and mode of involute coiling, e.g., Brightia oval with the maximum width at the dorsal svevi (Bonarelli), B. metomphala (Bonarelli). Our third. The flanks converge towards the venter, single fragment shows some similarity to a which is rounded and unicarinate. The conch is number of specimens attributed to these species; ornamented with umbilicolateral, short and weak however, for an undoubtable specific prorsiradiate ribs which strengthen at the dorsal identification more material from the same third of the flank in the form of tubercles or stratigraphic level is needed. bullae. Some bi- or trifurcate there into MATERIAL AND OCCURRENCE: (Type No. rursiradiate curved ribs turning adorally near the 1232A) M-7670 (coll. F. Hirsch), Makhtesh Hatira, venter where they disappear, leaving a smooth upper part of Be'er Sheva Formation, probably of venter. Sutures not preserved. Early Oxfordian age. DISCUSSION: This species is characterized by the i tubercle-like umbilicolateral ribs which bi- or trifurcate into finer, more densely spaced ribs. B. Brightia sp. B svevum is quite similar, differing by its non PI. 1, fig. 19 tubercle-like umbilicolateral ribs. B. metomphala DESCRIPTION: Two poorly-preserved fragments of is common in the Middle-Upper Callovian of an evolutely coiled planulate, unicarinate Brightia. Europe and Iran (Assereto et al., 1968) and only a U/D = 11.3/31.4 = 0.36. The ornament consists of few references are given herein in the synonymy broad, bullate, prorsiradiate umbilicolateral ribs (see: Lominadze, 1975). Lominadze (1975) included which bifurcate at the dorsal third of the flank in this species forms which develop long into adorally concave, rursiradiate ribs, finer than umbilicolateral ribs (ibid., PI. 2, figs. 2, 4), as the umbilicolateral ones. Sutures not preserved. w ell as variations in the ribbing density. He distinguished some of these variations as separate DISCUSSION: This form is quite similar to subspecies, following Tsytovitch (1911, in Brightia sp. A from Makhtesh Hatira (Israel), Lom in adze, 1975). According to the broad differing from it by finer ribbing. The broad ribs morphological range within metomphala s. st., of Brightia sp. A may be due to its state of there seems no justification for a separate preservation so that both forms from Israel and subspecies metomphalum multicostatum Tsytovitch. northern Sinai may be conspecific. Meanwhile, Hecticoceras metomphalum in Loczy (1915) has they are regarded separately and neither can be tubercle-like dorsolateral short bullae at the undoubtedly related to any recorded species. dorsal third of the flank, leaving the dorsal part MATERIAL AND OCCURRENCE: (Type No. 1232 of the adult stage smooth. Each such bulla B) M-7745(2) (coll. Z. Lewy), Gebel Maghara, top corresponds to 3-4 ribs, thus differing from our material. Zohar Formation. AGE: B. metomphala was recorded from Middle Brightia metomphala (Bonarelli) to uppermost Callovian beds (e.g., Jeannet, 1951, PL 1, fig. 20 p. 64; Lominadze, 1975, p. 37).

1919 Hecticoceras (Lunuloceras) metomphalum MATERIAL AND OCCURRENCE: (Type No. 1385) Bonarelli, Couffon, p. 187; PI. 14, fig. 7, M-7745(3) (coll. Z. Lewy), Gebel maghara, top text-fig. 29. Zohar Formation.

GSI Bull. 76, 1983 19 Z. LEWY U. CALLOVIAN AMMONITES

Brightia sp. cf. B. taeniolata (Bonarelli) MEASUREMENTS: PI. 1, figs. 23, 24

cf. 1975 Lunuloceras (Lunuloceras) taeniolatum D H W W/H U (Bonarelli, 1894), Lominadze,p. 79; PI. 8, figs. 1-3, M-7745:1 16.0 5.5(0.34) 5.1(0.32) 0.93 6.4(0.4) text-figs. 35-36. M-7745:1 25.5 11.0(0.43) 8.1(0.31) 0.74 10.0(0.4)

M-7745:2 - 10.8 9.3 0.86 DESCRIPTION: Two poorly preserved fragments of a compressed unicarinate conch with an M-774512 27.6 9.6(0.35) - - 11.0(0.4) umbilicus of approximately a quarter of the M-7745:3 - 12.9 11.4 0.88 conch's diameter. The ornament consists of ventrolateral, curved, rursiradiate ribs terminating at the ventrolateral shoulder. The dorsolateral region o f the flanks is smooth or irregularly ornamented by short rudimentary ribs, very few The umbilicus is large (U/D = 0.4). The o f which are strong and discernible as true ribs. whorl height is normally a little larger than its Sutures not preserved. width (W/H = 0.93-0.86) and a third of the DISCUSSION: Several Brightia species tend to diameter. shorten the dorsolateral ribs and, around the The ornament consists of falcoid ribs which umbilicus, form a smooth band which may be are strong and prorsiradiate near the umbilical slightly concave Ctaeniola" of Jeannet, 1951). The shoulder, where some bifurcate. They weaken at present fragments clearly show the absence of the dorsal third of the flank where they turn some umbilicolateral ribs, as well as the back and become stronger again, forming a curve occurrence of relics of such ribbing. By this concave adorally. The weakening of the ribs at ribbing pattern, as well as by the whorl section, their turning-point gives an impression of a our forms resemble Lominadze's (1975) Lunuloceras pseudo-furrow. taeniolatum. Unfortunately, their state of DISCUSSION: Our tricarinate specimens have a preservation does not enable a precise subangular whorl section thus differing from the determination. high triangular section of Campylttes. Jeannet (1951) indicated with a question mark the broad, tricarinate Putealiceras1 which are quite similar to AGE: B. taeniolata js recorded by Lominadze his Pseudobrightia. The specimens from Sinai are (1975, p. 80) from Lower Callovian to Lower more evolute than those from Switzerland Oxfordian strata. (Jeannet, 1951) and originate from an earlier biozone than the European ones and the MATERIAL AND OCCURRENCE: (Type No. 1391) specimens from Cutch (Spath, 1928). Our material M-7745(2) (coll. Z. Lewy), Gebel Maghara, top has the affinities of Pseudobrightia but because Zohar Formation. o f the fragmentary nature of the rather young ontogenetic stages, no new species is established genus PSEUDOBRIG HTIA Spath, 1928 here. For the same reason, the relations between our material and the 6 cm large Orbignyceras Type species: P. dhosaensis Spath, 1928 trezeense Gerard and Contaut of Collignon (1958) are not clear, although the partly exposed inner Pseudobrightia sp. volutions of the Madagascan species > closely PI. 1, figs. 7, 8 resemble our fragments. However, the holotype in ? 1958 Orbignyceras trezeense Ge'rard and Gerard and Contaut (1936; PI. 16, figs. 2,2a) has Contaut, Collignon, PI. 33, fig. 160. finer ribs than our specimen at the same stage.

AGE: Collignon's (1958) specimens originate from the Upper Callovian Athleta-Zone. DESCRIPTION: Evolutely coiled, planulate, with rather broad subquadrate adult whorl sections. The MATERIAL AND OCCURRENCE: (Type No. 1383) flanks are slightly rounded and subparallel and the M-7745(3) (coll. Z. Lewy), Gebel Maghara, top venter is rounded and tricarinate. Zohar Formation.

20 GSI Bull. 76, 1983 u. CALLOVIAN AMMONITES Z. LEWY

Subfamily DISTICHOCERATINAE Hyatt, 1900 DESCRIPTION: The Thamboceratidae are Genus DISTICHOCERAS Munier-Chalmas, 1892 characterized by oxycone unicarinate and bicarinate 'rype species: Ammonites bicostatus Stahl, 1824 conchs, having simple to very digitated sutures according to a basic pattern common to all of (= bipartitus Zieten, 1830) them. This pattern consists of a large first lateral Distichoceras bicostatum (Stahl) saddle of a rather bifid main part and an PI. 1, figs. 21, 22 external accessory saddle. The first lateral lobe is 1847 Ammonites bipartitus Zieten, d’Orbigny, p. narrow, followed by a bifid, narrow second 443; PI. 158, figs. 1, 2, 4. lateral saddle. The following three saddles up to 1928 Bonarellia bicostata (Stahl), Spath, p. 95; the umbilical seam are broad and low, separated PI. 15, figs. 4 a-c. by narrow lobes. 1928 Bonarellia sp. indet., Spath, p. 95; PI. 14, This pattern differs considerably from that of figs. 2 a-c. the Clydoniceratidae, which may have a very 1939 Distichoceras bicostatum (Stahl), Arkell, PI. broad first lateral lobe e.g., in Clydoniceras and 8, figs. 19 a-b.. Dhrumaites and a very broad second lateral 1951 Bonarellia bicostata Stahl, Jeannet, p. 36; saddle e.g., in Clydoniceras, Clydomphalites and PI. 8, figs. 1-5, text-figs. 81-82. Micromphalites. 1967 Distichoceras bicostatum (Stahl), Palframan, Within the Thamboceratidae a new genus, p. 62; PI. 9, figs. 1, 7, 8; PI. 11, figs. 3-5, 7, Levanticeras, is here designated. Thereby, the 8; PI. 12, figs. 3, 5-9; PI. 13, figs. 1-3; range of the family is extended to the Upper text-figs. 1-5, 7-9. Callovian. DESCRIPTION: A small fragment of an involutely coiled compressed conch. The venter is concave, Genus LEVANTICERAS nov. gen. bordered by ventrolateral clavi in alternating position. A siphonal keel occurs, lower than the HOLOTYPE: Levanticeras levantinense nov. gen. two rows of clavi. and sp. M-7813, (Type No. 1205), Makhtesh Hatira The ornament is very weak and is discernible (Israel, coord. 1490/0384), Upper Zohar Formation on the ventrolateral part of the flanks only. It (middle Tsia Member), PI. 2, figs. 1-3. consists of low ribs which bifurcate from the clavi dorsally, being slightly prorsiradiate. The pair DERIVATION OF GENERIC NAME: Distribution area. of ribs emerging from each clavi almost form a complete loop, but most of them fade and STRATIGRAPHIC LEVEL: Upper Callovian disappear before reaching the middle of the flank. DIAGNOSIS: Involute, compressed, oxycone with DISCUSSION: Spath (1928) and Jeannet (1951) acute venter. Low, falcoid narrow or broad ribs, recognized the priority of the name bicostatum slightly rursiradiate in the ventral half of the Stahl, 1824, for the same species commonly flanks, where bifurcation or short secondaries recorded as bipartitus Zieten, 1830, both may occur. Suture as described for the family. established on material from Wuttemberg, Germany. Being common, only a few references are herein given in the synonymy. Our specimen Levanticeras levantinense nov. gen. and sp. is the female type of Palframan (1967) who gave PI. 1, figs. 25-30; a broad synonymy for both dimorphs. PI. 2, figs. 1, 3, 4; Fig. 6 I, J.

AGE: This species seems to be restricted to the ? 1965 Clydoniceras sp., Abdallah, Adindani and Upper Callovian Athleta and Lamberti Zones Fahmy, p. 12. (Palframan, 1967, p. 92). 1975 Thamboceras sp., Gill and Tintant, p. 103. MATERIAL AND OCCURRENCE: (Type No. 1384) ? 1979 Nubidites omarai Wiedmann and Kullmann, p. 249; figs. 2,3. M-7745 (coll. Z. Lewy), Gebel Maghara, top Zohar Formation. HOLOTYPE AND STRATIGRAPHIC LEVEL: as for the genus. Superfamily STEPHANOCERATACEAE Neumayr, 1875 DERIVATION OF SPECIFIC NAME: Distribution Family THAMBOCERATIDAE Arkell, 1952 area.

GSI Bull. 76, 1983 21 Z. LEWY U. CALLOVIAN AMMONITES

exhibit a remarkable homoeomorphy (therefore DESCRIPTION: Involute, very compressed, Lewy, 1981, recorded the Israeli specimen as discoidal conch. Whorl section lanceolate with an Levanticeras pseudodiscus (Arkell) nov. gen.). acute venter throughout ontogeny (PI. 2, fig. 3). Arkell (1952, p. 282) noticed the similarity The maximum width is usually near the of the sutures of C. pseudodiscus to those of umbilicus, but in specimen M-5385, it occurs at Thambites forms which "seem to be inseparable mid-height. The flanks converge ventrally without from Clydoniceras” (Arkell, 1952, p. 279). These forming any ventrolateral shoulder, except in the close relations led Arkell (1952, p. 283) to suggest very young stage. The umbilicus in young stages that the "Clydoniceratidae are derived from is small (at D = 18, U = 2 mm; PI. 1, figs. 29, Tham bites and the Bajocian Thamboceras." 30) but with growth it is occluded by the dorsal However, the thamboceratid suture of Levanticeras part of the shell (PI. 2, fig. 3). nov. gen. strengthens the characteristics of this MEASUREMENTS: pattern, clearly differing from typical D H W/H Clydoniceras, and extends the range of the

M-7814 - 4.0 2.8 0.70 Thamboceratidae to the Upper Callovian. Collignon (1958; PI. 25, fig. 102) recorded a M-7814 13.8 8.0(0.58) 3.8(0.28) 0.47 1.8(0.13) Lower Callovian, oxycone, young ammonite under M-7814 18.3 10.4(0.57) 4.8(0.26) 0.46 2.0(0.11) Pseudoclydoniceras besairiei, having simple suture M-7813:1 47.5 28.2(0.59) 7.6(0.16) 0.27 lines. However, the lack of a precise suture

M-7813:1 - 86.0 30.0 0.35 pattern does not enable placing it conclusively as a forerunner of the Upper Callovian thamboceratid The young conch (D = 20 mm, PI. 1, figs. Levanticeras nov. gen., or as a post-Bathonian 29, .30) has ventrolateral radiate to slightly clydoniceratid. rursiradiate ribs, which weaken dorsally; with Gill and Tintant (1975) mentioned growth (D = 4-5 cm; PI. 1, fig. 25), the ribs Thamboceras sp. from the type locality of broaden, being adorally convex and rursiradiate Levanticeras nov. gen., which seems to be on the ventral margins. There a few secondaries nothing else but the latter new genus. Abdallah et seem to intercalate whereas some of the al. (1965) recorded from Jurassic outcrops at primaries bifurcate (inconclusive observations due Abu Darag, western side of Gulf of Suez, Egypt, to the state of preservation). This ventrolateral Clydoniceras with Erymnoceras and nearby ribbing is very weak and easily affected by Pachyceras, recalling assemblages of northern corrosion. Moreover, also the broad, lateral, Sinai and Makhtesh Hatira. Wiedmann and rursiradiate ribs occur on well-preserved specimens Kullmann (1979) described a very young oxycone only (PI. 1, fig. 26). ammonite from within the Nubian Sandstone The sutures (Fig. 6 I,J) have open sequence a few kilometers east of Abu Darag. (quadrangular) elements as in Thambites but a few They attributed it to a new genus and species, specimens may have "tree"-shaped first and second Nubidites omarai of Cretaceous affinities. The lateral saddles and the lobe in between with suture of this early ontogenetic stage (D = 11 narrow necks, resembling the suture of L. sinaiense mm) closely resembles the Thamboceratid pattern nov. gen. and sp. (Fig. 6 F). of the young Levanticeras nov. gen. (Fig. 6 J), DISCUSSION: Our oxycone specimens have a suggesting that Nubidites omarai and most typical thamboceratid suture with narrow first probably the Clydoniceras of the Abu Darag region are the present Upper Callovian lateral lobe and second lateral saddle, and broad umbilical saddles. Thereby Levanticeras nov. gen. Levanticeras nov. gen. However, additional as well as Clydoniceras pseudodiscus Arkell specimens and stratigraphic data of the Egyptian (Bathonian of central Saudi Arabia) differs from material are needed to prove this identity. typical Clydoniceras which tends to a very broad first lateral lobe. MATERIAL AND OCCURRENCE: Holotype (Typ« Levanticeras nov. gen. is a weakly ribbed No. 1205) M-7813:l and specimens M-7813(2), ammonite found together with Upper Callovian 5362(2), 5385, 5375, 7814 (coll. M. Goldberg, M, forms (e.g., Pachyerymnoceras). Therefore, it is Raab, F. Hirsch, Z. Lewy) Makhtesh Hatira distinguished from the Bathonian (associated with Upper Zohar Formation (upper part of Tsii Thambites), smooth (A rk ell, 1952, p. 282) Member). M-7621(10), 7663 (coll. Z. Lewy), Gebe Clydoniceras pseudodiscus Arkell, although both El-Minshera, (units 5, 6).

GSI Bull. 76, 1983 22 u. CALLOVIAN AMMONITES Z. LEWY

Levanticeras sinaiense nov. gen. and sp. and pers. comm., 1981) regards Pacherymnoceras PI. 2, figs. 5, 6; Fig. 6F as the microconch of Pachyceras. However, Charpy and Thierry (1977) distinguished in each of HOLOTYPE: M-7261:l (Type No. 1206), Gebel the taxa Pachyceras and Pachyerymnoceras a pair El-Minshera coord. 9690/0219); PI. 2, figs. 5-6; of micro- and macroconchs although they Fig. 6F. regarded Pachyerymnoceras as a subgenus of Pachyceras. DERIVATION OF NAME: Type area, Sinai. No definite dimorphic relations in the sense STRATIGRAPHIC LEVEL: Upper part of Zohar of Callomon or Charpy and Thierry could be Formation at Gebel El-Minshera, unit 5, the attributed to our specimens, although both lithostratigraphic equivalent of the Tsia Member Pachyceras and Pachyerymnoceras forms usually of Upper Zohar Formation in Israel, Upper occur together in Israel and Sinai. Likewise, no Callovian. Pachyceras lalandeanum (d'Orbigny) microconchs of Charpy and Thierry (1977) have been found with DIAGNOSIS: Levanticeras with low, fine and our "macroconchs." Our small number of dense ribbing, rather digitated sutures, with specimens of a rather high variability permitted "tree"-shaped elements. grouping them into several morphotypes only, DESCRIPTION: Involute, compressed, discoidal; without defining intraspecific variations or whorl section high, oxycone with a sharp venter dimorphism. If dimorphism occurs among our (fragmentary specimen). Pachyceratidae, it would most likely be between Pachyerymnoceras philbyi (A rk ell) as the MEASUREMENTS: macroconch and Pachyerymnoceras levantinense D H W W/H U nov. sp. as the microconch. However, due to the M-7261:1 - 15.7 6.3 0.40 state of preservation of our material, each

M-7261:1 44.0 31.0(0.70) 11.5(0.26) 0.37 2.3(0.05) morphotype is herein distinguished as a species of one of the two genera, either Pachyceras or The shell is ornamented by very low, slightly Pachyerymnoceras. falcoid, radiate fine ribs which fade and are almost invisible at the dorsal region of the flanks. The partly preserved ribbing pattern seems Genus PACHYERYMNOCERAS Breistroffer, 1947 to be of long primaries with one or two shorter secondaries in between, some of which probably Type species: Pachyceras jarryi R. Douville', 1912 furcate from the primaries. REMARKS: R. Douville' (1912, p. 37) distinguished The sutures (PI. 2, fig. 5, Fig. 6 F) comprise a globose Pachyceras-like, tuberculated Upper rather denticulated elements. The first lateral Callovian form as Pachyceras jarryi, discussing in saddle is broad with an external accessory saddle. detail its relations to both the Middle Callovian The first lateral lobe is deep and almost closed Erymnoceras and the Upper Callovian Pachyceras. by the adjacent tree-shaped second lateral saddle. The young stage resembles Erymnoceras by the The second lateral lobe is similar to the first cadicone whorl section and tuberculated umbilical one, but smaller. The following three saddles up shoulder, whereas advanced growth stages attain to the umbilical seam are broad and bifid. whorl sections greater in height than width, with DISCUSSION: L. sinaiense nov. gen. and sp. has a weakening of the tuberculation, thus resembling fine, dense ribs in contrast to the broad, widely Pachyceras. On the basis of these affinities, spaced ribs in L. levantinense nov. gen. and sp. Breistroffer (1947, in Arkell, 1957) regarded this Late Callovian taxon as a subgenus of the MATERIAL AND OCCURRENCE: M-7621(3) (coll. Middle Callovian Erymnoceras which, in the Z. Lewy), Gebel El-Minshera, Upper Zohar evolutionary sense, is unnecessary and Formation, unit 5. stratigraphically misleading. This may have influenced Imlay (1970) to attribute his Erymnoceras (Pachyerymnoceras) cf. E. (P .) jarryi Family PACHYCERATIDAE Buckman, 1918 to the Middle Callovian, although it occurs The Pachyceratidae comprise forms which are together with Pachyceras (similar biostratigraphic thought to be the macroconch and the microconch mixture in Gill and Tintant, 1975). of the same "biological" species. Callomon (1963; Zeiss (1974) discussed the ages of the

GSI Bull. 76, 1983 23 Z. LEWY U. CALLOVIAN AMMONITES undoubtable Pachyceras and Pachyerymnoceras fig. 10). Ribbing continues more or less in the species, some of which are accompanied by same width and spacing as in the preceding stage, so-called Erymnoceras-like ammonites. Attributing giving the impression of dense ribbing on the Arkell's (1952) Erymnoceras philbyi to large body-chamber. Pachyerymnoceras, he suggested that the Middle The third morphotype comprises the gerontic Callovian ammonite assemblages of Jebel Tuwaiq, part of the body-chamber. A sudden coarsening in Saudi Arabia (and thus its biostratigraphic ornament occurs there, forming simple or equivalent in Israel described herein) are of Late bifurcating, widely-spaced, strong and broad ribs Callovian age. (PI. 2, fig. 7, the most complete specimen from Saudi Arabia, refigured from Imlay, 1970). The dimensions of the shell at which each Pachyerymnoceras philbyi (Arkell) morphological change occurs, as well as the PI. 2, figs. 2, 7; PI. 3, fig. 10; Fig. 4 E dimensions of the complete adult conch, vary from specimen to specimen. Variations similarly 1952 Erymnoceras philbyi Arkell, p. 290; PI. 29, occur in whorl width to height ratio. figs. 1-3. A large fragmentary specimen from Gebel 1952 Erymnoceras cf. jarryi R. Douville', p. 290; El-Minshera, (M-7809), is more than twice as PI. 29, fig. 4. wide as the complete Erymnoceras cf. E. philbyi 1958 Erymnoceras aff. dorothea Spath, Hudson, p. Arkell, from Saudi Arabia (Imlay, 1970; refigured 418. herein in PI. 2, fig. 7) and its reconstruction 1970 Erymnoceras cf. E. philbyi Arkell, Imlay, p. makes it twice as large. The sutures are not D12; PI. 2, figs. 12-13. well preserved. DESCRIPTION: Large to moderately sized conchs, with three different types of morphology changing DISCUSSION: This species differs from P. rather suddenly at various diameters. The first levmtinense nov. sp., mainly by the densely ribbed morphotype, which resembles Erymnoceras, Pachyceras-like adult body-chamber. The comprises the whole phragmocone of the adult Erymnoceras-like phragmocones of both species stage in most samples. The second is may look similar, although that of P. levanttnense characterized by quite a high rounded whorl nov. sp. has a higher W/H ratios (1.8-2) with a section, densely ribbed like the preceding flatter venter and a sharper umbilical shoulder morphotype. In the third morphotype the ribs than in P. philbyi (W/H = 1.5), especially in become widely spaced and simple near the advanced growth stages. gerontic aperture. Spath (in Hudson, 1958) may have compared The first (young) morphotype is involute, the Israeli P. philbyi to his Erymnoceras cadicone and coronate. The venter and the flanks dorotheae, which occurs in Cutch in Upper form a complete arch (curved stronger than in P. Callovian strata. Because of its shape and the levanttnense nov. sp.) with W/H ratio of 1.5 (Fig. high stratigraphic position, Zeiss (1974) attributed 4 E). The umbilical wall is steep, slightly the species dorotheae to Pachyerymnoceras. rounded and quite smooth, except for low P. dorotheae (Spath, 1928, PI. 18, fig. 4) is undulations near the umbilical tubercles. The a small (young?) specimen which exhibits the umbilical shoulder is almost angular at the f/ymnoceras-like morphology and has a constricted tubercles and rounded in between them. The aperture. Because of its small dimensions, it is tangents at the umbilical region form nearly a impossible to decide whether this constriction straight angle between the umbilical wall and indicates the gerontic stage or the beginning of the umbilicolateral part of the flank. Low ribs bi- the mature one. The young stage of P. dorotheae or trifurcate from prominent umbilical tubercles. is similar to P. philbyi in whorl section and With growth, the tubercles become lower and ornament and only the doubtful morphology of fuse with the ribs emerging from them, forming the adult P. dorotheae impedes clarifying their short, broad ribs (or bullae). relations. Arkell (1952, p. 284) and Imlay (1970, p. The second (mature) morphotype comprises at D12) pointed out the remarkable homoeomorphy least half a volution of the body-chamber. It has a rather high whorl section due to a decrease in between their Middle Callovian Erymnoceras growth rate of the whorl's width relative to an (herein Late Callovian Pachyerymnoceras) and increase in its height, causing uncoiling (PI. 3, Bathonian Tulites of central Arabia. Even the

GSI Bull. 76, 1983 24 u. CALLOVIAN AMMONITES Z. LEWY bifid second lateral lobe by which Arkell (1952, MEASUREMENTS: p. 15, fig. 7) distinguished Tulites from D H W Erymnoceras does not seem to be a stable W/H U M- 5362 feature. Such bifid-like lobes occur in Erymnoceras - 25.5 47.3 1.8 - • (izjg., Jeannet, 1951, p. 116, figs. 263, 267) and in 91.2 37.7(0.41) 43.8(0.46) 1.2 29.8(0.32) some of our Pachyerymnoceras. It seems that • 113.1 39.4(0.34) 42.5(0.37) 1.1 40.5(0.35) the Arabian Tulites forms need further study on M-7663 - 24.0 40.6 - better preserved material that is stratigraphically 1.7 * more precisely sampled. 95.0 35.2(0.37) 43.3(0.45) 1.2 38.1(0.40) " Erymnoceras philbyi in the sense o f 98.0 32.5(0.33) 45.8(0.47) 1.4 42.2(0.43) Lominadze (1970) seems to be a true Middle M-53 28 - 19.2 38.6 2.0 - Callovian Erymnoceras sp. • - 33.8 56.4 1.6 - • MATERIAL AND OCCURRENCE: (Type No. 1208) - 43.0 58.0 1.3 - M-5340, 5362, 5313, 5346, ?6067 (coll. M. - - 55.0 55.0 1.0 _ Goldberg and M. Raab), Makhtesh Hatira; HU 30980 (coll. E. Nevo), Makhtesh Hazera; M-7809, DESCRIPTION: Inner whorls up to D = 6 mm 7621(3), 7909 (coll. Z. Lewy), Gebel El-Minshera. are smooth with a rounded umbilical shoulder. A ll samples from Upper Zohar Formation (Tsia With growth low umbilical bullae develop, which Member). at D = 16 mm become spinose and form the angular umbilical edge of the depressed cadicone (Teloceras-like) .whorl section. The conch is Pachyerymnoceras levantinense nov. sp. evolutely coiled, each volution embracing the PI. 3, figs. 1-9; Figs. 4A-D, F, 6G ventral part of the former volution nearly up to 1970 Erymnoceras philbyi Arkell, Imlay, p. D12; the umbilical shoulder. The venter of each PI. 2, figs. 3-9. volution forms a gentle curve, all being more or 1970 Erymnoceras (Pachyerymnoceras) cf. E. (P .) less parallel in cross-section (Fig. 4F). jarryi (R. Douvill^), Imlay, p. D13; PL 2, figs. The um bilical w all is steep, straight and 1- 2. quite smooth except for low undulations according 1974 Pachyerymnoceras imlayi Zeiss, p. 273; PI. to the position of the umbilical tubercules. The 37, figs. 5, 8-9. tangents to the umbilical wall and the ?1974 Pachyerymnoceras jarryi (R . Douville) umbilicolateral part of the flanks form a sharp ethiopicum Zeiss, p. 275; PI. 37, figs. 1, angle of approximately 60 -65 (PI. 3, figs. 6, 6-7. 8). The ribs bi- or trifurcate from the prominent umbilical tubercles situated on the almost sharp HOLOTYPE: (Type No. 1207) M-53621 (coll. M. angular umbilical shoulder. The ribs are gently Goldberg and M. Raab), Makhtesh Hatira, Zohar prorsiradiate, as broad as the interspace and Formation (Tsia Member, subunit 43 of Goldberg, rather low, so that in some specimens, they are 1963); PL 3, figs. 1-3. nearly erased on the middle of the venter. DERIVATION OF NAME: Levantine distribution A sudden morphological change occurs nearly area. at the end of the phragmocone and the beginning o f the body-chamber of the mature stage (at STRATIGRAPHIC LEVEL: Upper Callovian. diameters over 5-8 cm). The height of the whorl increases while the width may remain constant or DIAGNOSIS: Young stage, involute, very even decrease slightly at the region of depressed cadicone and coronate. Prominent morphologic change (PI. 3, fig. 2). The conch thus umbilicolateral tubercles from which low ribs bi- uncoils, becoming evolute (PI. 3, fig. 1). The adult or trifurcate and cross the venter. The adult stage has a high Pachyceras-like whorl section of stage is characterized by a sudden decrease or variable W/H ratios. The umbilical shoulder cessation in width growth with an increase in becomes rounded and the umbilical tubercles fuse the rate of height growth, resulting in uncoiling with the ribs and disappear. Ribbing becomes and a high Pachyceras-like whorl section. The widely spaced and stronger, tending to a simple adult and gerontic stages bear coarse and widely pattern toward single primaries on the gerontic spaced bifurcating or simple ribs. body-chamber. The largest preserved diameter is

GSI Bull. 76, 1983 25 Z. LEWY U. CALLOVIAN AMMONITES

nearly 12 cm whereas reconstructed conchs are 5394, 5393, 6067 (coll. M. Goldberg, M. Raab anc estimated to reach 15-16 cm. Z. Lewy), throughout the Tsia Member of th« The sutures preserved on two specimens show Zohar Formation; M-5416, ?6149 (coll. M, very broad, quadrangular (open) first and second Goldberg and M. Raab) at the base of the Be'et lateral saddles and rather narrow first lateral and Sheva Formation (Matmor Member). At Gebel umbilicolateral lobes (Fig. 6G). El-Minshera, units 5, 6: M-7621(10), 7663 (coll. R. DISCUSSION: This species is the most common Freund, Z. Lewy). among the Erymnoceras-like ammonites in the lower part of the outcrop of Makhtesh Hataira. However, its undoubtable distinction from young Pachyerymnoceras sp. cf. P. jarryi (R. Douville) stages of p. philbye is sometimes impossible. The PI. 4, fig. 3; PI. 5, fig. 1; Figs. 6B, H young stage of p. levantinense nov. sp. has a a f f . 1912 Pachyceras jarryi E. Eudes more depressed cadicone conch than P. philbyi, Desfcngchampe, R. Douvill^, p. 37; PL 1, figs. 3,4,5,7, but towards the adult stage, the whorl height of 8, 10; text-figs. 37-43. P. levantinense nov. sp. increases more rapidly a ff. 1977 Pachyceras (Pachyerymnoceras) jarryi than its width, thus becoming similar to P. (Douvill^) - Formemicroconque, Charpy and Thierry, philbyi. The adult P. levantinense nov. sp. lacks p. 206; PI. 5, figs. 2, 3; text-fig. 4d. the intermediate morphotype of P. philbyi with the densely ribbed, high Pachyceras-like whorls. DESCRIPTION: Involutely coiled, coronate, Erymnoceras species recorded from the depressed, globose conchs. In the adult stage the western side of the Gulf of Suez (Egypt; Abdallah height of the whorls increases more rapidly than et al., 1965) and from Makhtesh Hatira, Israel its width towards a Pachyceras-like section. (Gill and Tintant, 1975) could not be undubitably The edge of the umbilical shoulder bears attributed or compared to any of the tubercles from which low, rounded ribs bi- or Pachyerymnoceras species described here because trifurcate, being slightly prorsiradiate. The ribs no description or figure was presented. are as broad as their interspacing and cross the P. jarryi (according to R. Douville', 1912) does venter almost without any flexure. The growth not show the sudden morphological change in angle of the whorl's width is large in the young whorl section and ornament as does P. stages and decreases in the adult stage towards levantinense nov. sp., but rather a gradual an almost constant width, while the height increase in whorl height toward a Pachyceras-like increases. The largest specimen developed a section without uncoiling. triangular adult whorl section without any change P. jarryi ethiopicum Zeiss (1974) has a in ornament. compressed cadicone conch like P. levantinense Sutures (Fig. 6H) with a narrow bifid nov. sp., with rather fine umbilicolateral external lobe, a broad first lateral saddle followed tubercles and ribbing which may occur in P. by the small second lateral bifid lobe on the levantinense nov. sp. Also similar in shape is P. middle of the flank and the similarly wide sp. cf. P. jarryi of Imlay (1970) which differs second lateral bifid saddle. The umbilical lobe is from levantinense nov. sp. only in the adult stage just on the umbilical shoulder and its wall. by its gradually forming the triangular whorl DISCUSSION: Our specimens are closely related section. P. imlayi Zeiss seems to represent the to P. jarryi (R. Douville). The adult holotype of adult, coarsely ornamented stage of P. jarryi this species (Douville, 1912, PI. 1, fig. 10) is ethiopicum so that both Ethiopian forms are more compressed and reaches the Pachyceras-like believed to belong to P. levantinense nov. sp. The stage in smaller diameters than in our material, present new species is based on well- preserved, whereas the young stages of R. Douville (1912, complete conchs from Israel which the PI. 1, figs. 3-5, 7-6, 12) are very depressed and fragmentary material from elsewhere only partly more finely ribbed than our specimens. These resembles. Therefore, a new name was designated young stages, as well as the young Ethiopian P. to avoid possible misinterpretation of the foreign jarryi ethiopicum Zeiss (1974), resemble the young species not in hand. depressed conchs of levantinense nov. sp. This MATERIAL AND OCCURRENCES: (Type No. latter species is characterized by a sudden 1207) At Makhtesh Hatira, M-5302(2), 5304, 5324, change in morphology in the adult stage in 5326, 5328, 5333, 5362, 5371, 5372, 5375, 5384, contrast to the gradual change in P. jarryi. Our

26 GSI Bull. 76, 1983 Z. LEWY u. CALLOVIAN AMMONITES

Pachyerymnoceras sp. aff. P. jarryi does not were attributed to different species and genera show any change in ornament while forming the o f Middle Callovian to Late Callovian age. This Pachyceras-like whorl section as does P. taxonomical process (e.g., R. Douvill^, 1912; levantinense nov. sp. from Makhtesh Hatira L<5czy, 1915; Spath, 1928, p. 219; Arkell, 1957) (Israel), which can also be attributed to the overlooked the existence of cadicone present described species. Charpy and Thierry Erymnoceras-like species ranging into the Late (1977) regarded these forms of jarryi in Douville' Callovian, such as the present cf. coronoides (1912) as microconchs of a larger, more Quenstedt. L6czy (1915) has attributed it to compressed macroconch of the same species. Our Stepheoceras Buckman (1898, synonym of few specimens do not confirm their suggestion of Stephanoceras Waagen, 1869, in Arkell, 1957), dimorphism in this species. Lominadze (1970) included it in Erymnoceras, whereas the restriction of Erymnoceras to the A G E : P. jarryi, the type species of Middle Callovian only left this form without a Pachyerymnoceras is known from the Upper suitable generic name in Arkell's (1957) Callovian only (e.g., Arkell, 1957, p. L. 297). svstematics. This form is well known in Europe and now probably also in the Middle East, but it MATERIAL AND OCCURRENCE: (Type No. 1380) seems that no proper genus has been established M-7745(4) (coll. M. Goldberg), Gebel Maghara, top for it. Although it resembles early stages of Zohar Formation. Pachyerymnoceras, it is distinguished (at least for the time being) by the lack of any ontogenetic cf. ”Erymnoceras1 coronoides (Quenstedt) polymorphism in large specimens. Meanwhile, this PI. 4, figs. 1-2 partly known form is left under the generic name " E ry m n o c era s" in spite of the possible c f. 1848 Ammonites coronatus Bruguiere, stratigraphic misinterpretation. d'Orbigny, p. 465 (part); PI. 168, figs. 3, Our fragment seems to be the largest one 6, 7. recorded. This may be the reason for the cf. 1915 Stepheoceras coronoides Quenstedt, abundance of the trifurcating ribs in contrast to Loczy, p. 347; PI. 14, fig. 8. their rare occurrence on the small conchs of d'Orbigny (1848) and Ldczy (1915). DESCRIPTION: A single fragment of the last volution (part of the phragmocone and AGE: Typical E. coronoides Quenstedt are of a body-chamber) o f a large, depressed cadicone Middle Callovian age, whereas the Hungarian conch. The width to height (approximate height) specimen occurs in the Upper Callovian of ratio is 119/58 = 2.0. The venter is gently curved Hungary (L6czy, 1915). with rounded ventrolateral shoulders. Prominent umbilicolateral bullae stretch dorsally and weaken MATERIAL AND OCCURRENCE: (Type No. 1204) on the umbilical wall. These bullae furcate on the M-5302, (coll. M. Goldberg and M. Raab), venter into two or three low and narrow, radiate Makhtesh Hatira (Israel), Upper Zohar Formation, to slightly prorsiradiate ribs. The ribs cross the lower part of Tsia Member. venter and at least two of them join the opposite bullae. Occasionally, one rib of a bundle weakens Genus PACHYCERAS Bayle, 1878 before reaching the opposite ventrolateral shoulder. Type species: Am. lalandeanus d'Orbigny, 1848 The poorly-preserved sutures exhibit broad, DESCRIPTION: R. Douville' (1912) described the open, quadrangular elements, with saddles more ontogenetic polymorphism in P. lalandeanum. than twice as broad as the dorsally adjacent Recently, Charpy and Thierry (1977) gave a lobes. detailed description and illustrated the DISCUSSION: This Middle to Early Late Callovian polymorphism, regarding this large form as the form described and illustrated by Loczy (1915) is macroconch of a smaller, different-looking based on specimens attributed by d'Orbigny (1848, dimorph. This microconch shows gradual coarsening PI. 168, figs. 3, 6, 7) to the Middle Callovian of ornamentation on the gerontic body-chamber species coronatus Bruguiere. Under the same whereas the macroconch has three completely specific name, d'Orbigny (1848, Pis. 168-169) differing morphotypes during ontogeny. Our sparse presented a variety of morphotypes which later and fragmentary material lacks Charpy and

27 GSI Bull. 76, 1983 Z. LEWY U. CALLOVIAN AMMONITES

Thierryfe (1977) "microconch" of P. lalandeanum; Over a diam eter o f 8-9 cm, the flanks m oreover, it does not show any dimorphism converge towards an angular venter developing between Pachyceras and Pachyerymnoceras as with growth a lanceolate (or cordate) whorl suggested by Callomon (1963). Thus these forms section. In this adult stage (the gerontic are regarded herein as separate genera. phragmocone) the shell attains a discoidal shape (resembling Cardioceratidae) with a very narrow, rounded to nearly acute venter (in the internal Pachyceras spathi nov. sp. mould). PI. 5, figs. 2-4; Fig. 4 G The whorl section of the gerontic HOLOTYPE: Type No. 1249, M-7691:l (coll. M. body-chamber changes from lanceolate to sub-quadrate with subparallel flattened flanks and Raab), Makhtesh Hatira, base Be'er Sheva Formation, PI. 5, figs. 2-4, Fig. 4 G. a broad rounded venter accompanied by uncoiling. The gerontic aperture is slightly constricted. The DERIVATION OF NAME: In honour of L.F. Spath ribbing pattern of the shell changes step by step who studied the ammonites of Makhtesh Hatira (in with the change in whorl section and coiling. The Hudson, 1958). young conch has strong, slightly prorsiradiate ribs which bi- or trifurcate at the umbilical shoulder STRATIGRAPHIQ LEVEL* Upper Callovian. from short bullae. Occasionally, they are DIAGNOSIS: Large (D = 20 cm) Pachyceras, intercalated by shorter secondaries. The ribs are involute, rather compressed, having three shapes as broad as their interspaces and cross the throughout ontogeny. The young conch has a venter uninterrupted as strongly as on the flanks. broad, oval section with a rounded venter With growth, the ribs become lower but ornamented by strong ribs. The adult stage retain their width and interspaces as in the develops a high lanceolate whorl section earlier stage, giving an impression of dense ornamented by low, dense ribs; the gerontic ribbing on the large discoidal conch. The ribs body-chamber uncoils and returns to subparallel weaken before the narrow venter and do not flanks with a broad rounded venter ornamented by cross it. coarse, widely spaced ribs which fade and At the beginning of the gerontic body disappear adorally, leaving a smooth shell near chamber, the ribs suddenly coarsen and turn into the gerontic aperture. broad, low, simple ribs. Others unsuccessfully start to bifurcate, forming a broad triangular rib D ESC R IPTIO N: Involutely coiled, large, rather near the venter. The ribs cross the venter compressed conchs, attaining diameters over 20 forming low, broad undulations. Near the gerontic cm. The gerontic-body chamber uncoils aperture, the conch tends to constrict and the considerably. ornament disappears leaving a smooth shell along MEASUREMENTS: 5 cm (or more) before the aperture (PI. 5, fig. 2). The sutures are poorly preserved but show D H W W/H U broad, open first lateral and second lateral saddles M-7S11 - 40. 5 37 0.91 - and narrow, open first and second lateral lobes.

M-7691 114 '55.0(0.48) 47(0.41) 0.85 23(0.20) DISCUSSION: Pachyceras spathi nov. sp. is more " 160 74.0(0.46) 60(0.37) 0.80 28(0.17) compressed than P. tndicum Spath whose gerontic ■ body-chamber is unknown. P. lalandeanum ISO 77.0(0.42) 62(0.34) 0.80 34(0.19) (d'Orbigny) attains its lanceolate section at larger • 213 80.0(0.37) 64(0.30)* 0.80* 55(0.26) diameters than in P. spathi nov. sp., with a *reeon*t ruet»d more inflated whorl section with rounded flanks, differing from the rather triangular section in P. spathi nov. sp. P. lalandeanum usually differs from The young coach is founded to oval in P. spathi by its rather weak dorsolateral ribs, section, becoming discoidal-oval with growth due becoming stronger ventrally. to a more rapid increase in the height than in The reexamination of Obtustcostites of Spath the width of the whorls (Fig. 4G). The flanks (in Hudson, 1958) from the Eligmus-Grossouvria are rounded, converging towards a broad, rounded unit at Makhtesh Hatira (sample C-71700, British venter. The umbilicus is narrow and deep with Museum) suggests it to be a fragment of the steep walls and rounded umbilical shoulders. inner whorls of P. spathi nov. sp.

28 GSI Bull. 76, 198: u. CALLOVIAN AMMONITES Z. LEWY

Charpy and Thierry (1977) attributed to their DISCUSSION: This species (the macroconch in the P. lalandeanum d'Orbigny) macroconch a broad sense of Charpy and Thierry, 1977) is range of morphological variations. Although not characterized by a compressed, lense-shaped figured, it seems that they would have included conch without any umbilical tuberculation. It P. spathi nov. sp. in P. lalandeanum (Thierry, thereby differs from Pachyerymnoceras which 1981, pers. comm.). In the same sense, Gill and possesses umbilical tubercles and has depressed Tintant (1975) may have included it in their P. whorl sections in the young stages, becoming lalandeanum from Makhtesh Hatira (30 m above higher with growth into Pachyceras-like whorls. base Tsia Member into the lower 20 m of the Therefore, the Pachyceras lalandei of R. Douvill^ Be'er Sheva Formation). (1912, PI. 2, fig. 1) is herein excluded from this species due to its compressed young whorls, MATERIAL AND OCCURRENCE: Holotype probably with umbilical tubercles. This specimen is M-7691 (Type No. 1249) and specimens M-6003, thought to represent a Pachyerymnoceras, perhaps 5382, 5993, 6022 (coll. M. Goldberg and M. an advanced growth stage of P. jarryi (R. Raab) and M-7811* (coll. F. Hirsch and M. Douvill^). Goldberg), Makhtesh Hatira; all except M-5382, It is quite impossible to relate to the 5993 are from the base of the Be'er Sheva fragmentary young stage of cf. P. lalandeanum Formation (M-5382, 5993 not in situ in the upper part of the Zohar Formation). (d'Orbigny) of Zeiss (1974) or to the unfigured P. lalandeanum recorded from Makhtesh Hatira (Israel) by Gill and Tintant (1975). This latter form, as well as the herein described new Pachyceras lalandeanum (d'Orbigny) species P. spathi or the Pachyceras sp., may be PI. 4, fig. 4; Fig. 5A from the same locality. As Spath (1928) stated, 1848 Ammonites lalandeanum d'Orbigny, p. 477; his Pachyceras indicum is closely related to the PI. 175, figs. 1-3, non 4-5. European P. lalandeanum. P. indicum has less 1912 Pachyceras lalandei d'Orbigny, R. Douvill^, rounded flanks and thus a triangular whorl section p. 44; PI. 2, figs. 2, 3, 5, non 1; text-figs. without an acute venter. P. spathi nov. sp. 32, 47-51. already attains a lanceolate section in smaller 1977 Pachyceras (Pachyceras) lalandeanum diameters than P. lalandeanum and thereafter (d'Orbigny) - Forme macroconque, Charpy and recoils and forms the gerontic body-chamber with Thierry, p. 204; PI. 1; PI. 2, fig. 2; PI. 4, fig. the broad, rounded venter. The ribs of P. spathi 2; text-fig. 4c. nov. sp. are less prorsiradiate than in P. lalandeanum and tend to start at the umbilical DESCRIPTION: Involutely coiled, lense-shaped shoulder, whereas the ribs of P. lalandeanum large conchs. The young stage has a broad and weaken and usually disappear before reaching the rather circular whorl section becoming higher umbilical shoulder. than wide with growth (Fig. 5A). The flanks converge gradually toward the rounded venter AGE: Pachyceras lalandeanum (d'Orbigny) appears which becomes narrower and almost acute in the in Europe in the upper part of the Athleta-Zone adult stage with weak ventral shoulders, thus and is most abundant in the Lamberti-Zone, both attaining a lanceolate whorl section. of Late Callovian age (e.g., Charpy and Thierry, 1977). The ornament of the young stage consists of prorsiradiate ribs which tend to fade and become MATERIAL AND OCCURRENCE: (Type No. 1386) narrower dorsally, leaving a smooth umbilical M-7745(6), 7746 (coll. M. Goldberg and Z. Lewy), shoulder. Most ribs are primaries, but secondaries Gebel Maghara; M-7852 (coll. Z. Lewy), Gebel may occur, all crossing the venter with an El-Minshera, top Zohar Formation. adorally convex arch. In the adult stage the ribs end before the acute venter and contribute thereby to the formation of the ventral shoulder. Pachyceras magharense nov. sp. The umbilicus is rather small with a deep, steep, PI. 6, fig. 12; Fig. 5B smooth umbilical wall in all stages. In a few specimens the ribs start from the umbilical cf. 1977 Pachyceras (Pachyceras) lalandeanum shoulder but they do not form tubercles or (d'Orbigny) - Forme macroconque, Charpy and bullae-like inflations there. Thierry, p. 204; PI. 2, fig. 1.

GSI Bull. 76, 1983 29 Z. LEWY U. CALLOVIAN AMMONITES

HOLOTYPE: M-7745 (Type No. 1392), Gebel P. lalandeanum (macroconch) a coarsely ribbed Maghara, northern Sinai (coll. M. Goldberg et al., variety which very much resembles our specimen 1971, at their subunit 82), PI. 6, fig. 12, Fig. 5B. although the French one does not show the high acute keel of the lanceolate phragmocone seen DERIVATION OF NAME: Type locality. in our material. STRATIGRAPHIC LEVEL: Top Zohar Formation, MATERIAL AND OCCURRENCE: (Type No. 1392) Upper Callovian. M-7745 (coll. M. Goldberg), Gebel Maghara, top DIAGNOSIS: Involute, recoiling in the gerontic Zohar Formation. stage. Adult conch lenticular, whorl section lanceolate with an acute venter, becoming rounded in the gerontic stage with an inflated Pachyceras crassum R. douville' whorl section. Strong, coarse prorsiradiate ribs, PL 4, fig. 5; Fig. 6A weak or absent on the ubilical region, forming ? 1848 Ammonites lalandeanum d'Orbigny, p. 477; chevrons on the gerontic venter. PI. 175, figs. 4-5. ? 1912 Pachyceras crassum R. Douvill^, p. 42; DESCRIPTION: A single, almost complete PL 1, figs. 1-2, 9, 11; PI. 2, fig. 4, text-figs. specimen of an involutely coiled, lenticular conch 45-46. exposing the adult and gerontic stages only. The ? 1916 Pachyceras cf. lalandei d'Orbigny, H. adult stage has a lanceolate whorl section with a Douvill^, p. 70; PI. 8, figs. 4-5. high, acute venter and differentiated ventrolateral 1977 Pach ycera s (Pachyceras) lalandeanum shoulders at the endings of the strong ribs. The (d'Orbigny) - Forme microconque, Charpy and umbilicus is small (U/D = 30/170 = 0.17) with Thierry, p. 202; PL 5, fig. 1, text-fig. 4b. rounded shoulders and a steep wall. The gerontic stage is marked by recoiling (U/D = 48/210 = DESCRIPTION: Involutely coiled, globose and 0.23) and by the inflating of the whorl section depressed section in the young stage, increasing forming a broad, rounded venter. The gerontic the growth rate of the height relative to the aperture is constricted. The adult and gerontic width toward an oval section. The umbilicus is stages are ornamented by coarse, prorsiradiate small and very deep with steep and smooth ribs, as broad as their interspaces. They are umbilical walls and rounded shoulders (Fig. 6A). weak or completely absent near the umbilicus, The conch is ornamented with rounded ribs as becoming stronger ventrally. At the ventrolateral broad as their interspacing. These are narrow region they are most pronounced and weaken on and rather weak near the umbilicus becoming the venter so that a ventrolateral shoulder is broader and stronger toward the venter in a formed. The ribs on the gerontic body-chamber slightly prorsiradiate pattern. Shorter secondaries cross the rounded venter forming chevrons there. sometimes intercalate the primaries. No umbilical Sutures not preserved. tuberculation occurs superimposed on the ribs, which begin on the umbilical shoulder. The DISCUSSION: The shape of the early stages of spacing of the ribs increases gradually with this form is unknown. Although the adult stage growth but the ribs remain rather low and has a lanceolate whorl section reminiscent of a rounded throughout ontogeny. The gerontic stage is Pachycardit eras, this species is attributed to missing in our specimens. Pachyceras on the basis of the morphological development of this latter genus as well as DISCUSSION: Our material closely resembles that because of our lack of records on such large, o f R_ Douvill^ (1912) in its whorl sections and coarsely ornamented Pachycardioceras species from ornament. The weak umbilical tuberculation Late Callovian or even Early Oxfordian rocks. discernible in his PI. 2, fig. 4, may be the P. magharense nov. sp. differs from all other starting points of the ribs. The umbilical region Pachyceras species by its lanceolate adult whorl of P. lalandei in R. Douvill^ (1912) in PI. 2, fig. section with the high acute venter and the coarse 1 is not clear. If the tubercle-like structures are ornament. The gerontic body-chamber may really superimposed on the ribs this specimen resemble that of P. spathi nov. Sp., although the should be attributed to' Pachyerymnoceras; but latter has bifurcating ribs forming triangular broad if these are only the starting points of the ribs inflations because both branches are close to then this globose form is a P. crassum. Similarly each other. Charpy and Thierry (1977) included in there is a question of identity of the depressed

30 GSI Bull. 76, 1983 u. CALLOVIAN AMMONITES Z. LEWY fragment of P. cf. P. lalandei of H. DouvilM Pachyceras robustum nov. sp. (1916). This globose Pachyceras species of an PI. 5, figs. 5, 6; PI. 6, fig. 1 unknown gerontic conch has been attributed by H O LO TYPE: Type No. 1390, M-7745, Gebel Charpy and Thierry to the microconch of P. Maghara, northern Sinai (coll. Z. Lewy); PI. 5, fig. talandeanum. Our material reaches diameters over 6; PI. 6, fig. 1. 11 cm without any sign of senility as seen in the French specimens, which do not exceed 10 cm. DERIVATION OF NAME: Morphological affinity. It seems that globose Pachyceras macroconchs in STRATIGRAPHIC LEVEL: Top Zohar Formation, the sense of Charpy and Thierry (1977) occur Upper Callovian. alongside the globose microconchs which may look similar in the young ontogenetic stages. This DIAGNOSIS: Involute, globose, cadicone conchs, assumption is supported by the triangular whorl whorl height increases more rapidly than the section of our large specimen which width forming a triangular whorl section. Strongly characterizes the second ontogenetic stage of prorsiradiate ribs furcate from low umbilical Pachyceras ("macroconchs"). Due to the unknown tubercles, forming chevrons on the venter. gerontic body-chamber of this globose form it is DESCRIPTION: Involutely coiled, globose conchs. herein distinguished from wide P. lalandeanum. The flanks are gently rounded and converge AGE: Pachyceras crassum (R. Douvill^ (1912) is towards the rounded venter forming together a an Upper Callovian species. triangular whorl section. The umbilical shoulder MATERIAL AND OCCURRENCE: (Type No. 1387) is sharp and angular and the umbilical wall is M-7745(2), 7746 (coll. Z. Lewy), Gebel Maghara steep. The umbilicus is cone-shaped and deep. region, top Zohar Formation. MEASUREMENTS:

D H W W/H U

M-7745:1 48.5 23.0(0.48) 37.0(0.76) 1.6 13(0.27) Pachyceras sp. M-7745;l 121.0 62.0(0.50) 80.0(0.66) 1.3 28(0.23) PI. 6, fig. 2; Fig. 6C The umbilical shoulder is damaged in most DESCRIPTION: Two young specimens (D = 14, 30 specimens, but in one fragment it bears mm), partly corroded. Moderately evolute. The tubercles from which weak and narrow whorl section of the inner volutions is rounded (H prorsiradiate ribs furcate. They become broader = W) becoming cordate with growth with the and stronger ventrally, intercalated occasionally by width slightly greater than the height (Fig. 6C). secondaries. The ribs curve adorally, forming The young stage is smooth with sproadic rounded chevrons on the venter. Sutures not constrictions and irregular, prorsiradiate, weak preserved. ribs. Ribbing strengthens with growth especially on the venter and ventrolateral region, weakening DISCUSSION: This form resembles some globose dorsally towards a smooth umbilical shoulder (D = Goltathttes or Herznachites species of the 30 mm). Suture not preserved. Cardioceratinae by the triangular whorl section and the strongly prorsiradiate ribs, forming chevrons on the venter. However, the ribs are quite straight and not falcoid, and the young DISCUSSION: The mode of coiling, whorl section stages of. our specimens have no sign of an acute and ornament suggest that this young form belongs to Pachyceras rather than to the venter as in most Cardioceratinae. On the other involute, coronate Pachyerymnoceras. However, due hand, it d iffe rs from the recorded to the lack of adult forms an undoubtable generic Pachyerymnoceras species by the strongly identification is impossible as is its relations to prorsiradiate ribs and by the absence of any morphological changes up to its largest diameter other Pachyceras species. o f 13 cm. The whorl section and the ribbing resembles those found in some Pachyceras, but MATERIAL AND OCCURRENCE: (Type No. 1367) this latter genus usually lacks umbilical tubercles, M-5339, 5351 (coll. M. Goldberg and M. Raab), which occur in our material. Similar tuberculation Makhtesh Hatira, upper part of the Zohar and prorsiradiate ribbing occur in Pachyceras Formation (middle Tsia Member). lalandei of R. Douvill^ (1912, PI. 2, fig. 1) which

GSI Bull. 76, 1983 31 Z. LEWY U. CALLOVIAN AMMONITES

is more compressed than our large specimen. Our imprint o f the inner1 volution shows a broad largest specimen shows some of the affinities of venter (dorsum of the present fragment in Fig. the Pachyceratidae, however, there is some doubt 6D). W/H decreases with growth and the venter as to whether it is a large, young specimen becomes carinate. which would have undergone the same MEASUREMENTS: morphological changes that are typical to Pachyceras ("macroconch"). H W W/H A fragment (M-5450) from the upper part of M-7261 :1 7.3 7.8 1.7 the Zohar Formation at Makhtesh Hatira (not in situ) resembles this species in whorl section and M-7261:1 8.7 7.8 0.9 strongly prorsiradiate ribbing. Because of its bad state of preservation, it is only tentatively Ornament o f prorsiradiate, slightly sigmoidal, attributed to this species. bifurcating low ribs forming chevrons on the MATERIAL AND OCCURRENCE: (Type No. 1390) sharp venter. Sutures not preserved. M-7745(4) (coll. Z. Lewy), Gebel Maghara, top DISCUSSION: The cordate whorl section of the Zohar Formation and probably M-5450, Makhtesh small fragment and the mode of ornament Hatira, upper Upper Zohar Formation. resemble those occurring in some Quenstedtoceras. However, they do not even enable undoubtable generic identification. Family CARDIOCERATIDAE Siemiradzki, 1891 MATERIAL AND OCCURRENCE: (Type No. 1305) REMARKS: Several of the ammonites studied M-7621(2) (coll. Z. Lewy), Gebel El-Minshera, unit show morphological affinities of the 5, Upper Zohar Formation. Cardioceratidae. None o f the recorded genera in the available literature completely fits the description of our material. However, the Genus LAMBERTICERAS Buckman, 1920 specimens may be compared to quite similar looking genera to avoid the definition of new taxa Type species: Am. lamberti J. Sowerby, 1819 based on incomplete m aterial (e.g., lack of cf. Lamberticeras henrici (R. Douvilll) sutures). Both Thierry and Callomon (pers. comm., PL 7, figs. 1-6 1981) suggested regarding these forms as new genera (or dimorphs of known genera) to avoid cf. 1912 Quenstedticeras henrici R. Douvill^, p. any relations with the European Quenstedtoceras, 55; PL 4, figs. 24-33. Lamberticeras and Prorstceras, hitherto unknown cf. 1972 Quenstedtoceras henrici (R. Douville), from the southern Tethyan region, due to which Reyment, p. 20; PI. 2. the Lamberti Zone could not be recognized there DESCRIPTION: Moderately evolute, planulate (Callomon, 1962, p. 274). However, the remarkable small (D < 5 cm) conchs. The exposed volutions, D > 2 similarity of our specimens to these European cm, have flanks converging gently towards a low, genera, as well as their suitable stratigraphic acute venter. level led to the usage, with appropriate caution, of these Boreal generic names. Better preserved MEASUREMENTS: specimens of these Cardioceratid-like ammonites D H W W/H U will clarify their identity as well as their M-5397 30.0 12.0(0.4) 9.3(0.31) 0.77 9.1(0.33) correlation to European genera. M-5346 32.5 13.0(0.4) 8.1(0.25) 0.62 10.6(0.32)

Genus QUENSTEDTOCERAS Hyatt, 1877 The ornament (over a diameter of 2 cm) consists o f prorsiradiate bifurcating ribs becoming more Type species: Am. leachi J. Sowerby, 1819 widely spaced with growth. They are rather weak "Quenstedtoceras1 sp. near the umbilicus and the middle of the flanks, PI. 7, fig. 7; Fig. 6D become stronger and arch forward near the venter. The ribs cross the acute venter forming DESCRIPTION: Two small fragments of an chevrons with a lower pseudocarina in between evolute conch with a cordate whorl section. The them. Sutures not preserved.

32 GSI Bull. 76, 1983 u. CALLOVIAN AMMONITES Z. LEWY

DISCUSSION: Lamberticeras henrtci R. Douvill^ DIAGNOSIS: Small (D < 3 cm), quite evolute, (1912) is characterized by bifurcating ribs with planulate conch. Young stage smooth attaining occasionally a single secondary in between the with growth strongly prorsiradiate bifurcating ribs, primaries. Thereby it differs from L. lamberti which become coarser with age and form chevrons which usually has two or three secondary ribs on the gerontic venter. Straight projecting ventral between the simple or bifurcating primaries. The rostrum. whorl section of L. lamberti and L. praelamberti DESCRIPTION: The mature holotype has a (R. Douvill^) is highly cordate with a sharp venter diameter (before the rostrum) of 23 mm and the at diam eters o f 3-5 cm, thus differing from largest, almost complete specimen (M-5384) has a henrici which tends to rounding of the venter diam eter of 30 mm. The whorl section has with growth. sub-parallel flanks and a rounded venter which Our specimens resemble L. henrici in whorl may be fastigate in the young ontogenetic stage. section and ornament, although differ from some of the specimens from France and Scandinavia MEASUREMENTS: (Reyment, 1972) and British Columbia (Frebold and D H W W/H U Tipper, 1975) by weaker dorsolateral ribbing in M-6089 23.0 7 .5 (0 .3 2 ) 6.0(0 .26 ) 0.80 7.7(0.33) addition to the following features: M-5397 tends Holotype to coarse and widely spaced ribbing at D>25 mm M-5384 25.0 8.8 (0 .3 5 ) 7.3(0 .29 ) 0.83 9.2(0.37) (early maturity?); M-5346 is flattened like the French L. praelamberti, but is more coarsely * 30.0 10.2(0.34) 8.0(0.27) 0.78 11.8(0.39) ribbed. Due to the intraspecific variability seen in the material figured by R. Douville' (1912, PI. The conch becomes evolute with growth (U/D 4), more well-preserved material is needed to = 0.33-0.39) whereas the W/H ratios slightly clarify the identity of the Israeli specimens, decrease. The venter is relatively obtuse and even which have meanwhile been attributed to the rounded in the mature stage, but it may be closest-looking form. fastigate, with a pseudo-carina in between the strongly prorsiradiate ribs which converge towards AGE: L. henrtci R. Douvill^ characterized the the venter. The gerontic complete specimen (D = lower subzone of the Late Callovian 23 mm) has a straight, projecting ventral Lamberti-Zone (Callomon and Sykes, in: Duff, rostrum in the form of a smooth scoop 1980). characteristic to Quenstedtoceras. The young MATERIAL AND OCCURRENCE: Specimens (Type conch is smooth up to a diameter of 9-12 mm, No. 1209) M-5346, 5397 (coll. M. Goldberg and M. where it starts to develop weak, broad, prorsiradiate ribs. Some of the ribs bifurcate at Raab), Makhtesh Hatira, Upper Zohar Formation the dorsal third of the flank, but most of them (Tsia Member); at Gebel El-Minshera (coll. Z. are singles with a shorter secondary one in Lewy), M-7621(2) unit 5, and M-7852 unit 7 between. A ll ribs cross the venter forming uppermost part of Zohar Formation. chevrons. Ribbing becomes coarser near the gerontic aperture, strengthening the chevrons on the venter (PI. 6, figs. 8, 10). Sutures not Genus PRORSICERAS Buckman, 1918 preserved.

Type species: Ammonites gregarius Leckenby, DISCUSSION: "P ." hatirae sp. nov. comprises sm all specimens with a simple ribbing pattern of 1859 bifurcating, or alternating primary and a single " Prorsicerad1 hatirae sp. nov. secondary rib, thus differing from the larger, more PI. 6, figs. 7-11 complexly ribbed P. gregarium (Leckenby, 1859 in Arkell, 1957). The Israeli material shows the HOLOTYPE: (Type No. 1210) M-6089 (coll. M. presence of a rostrum such as known from Goldberg and M. Raab), Makhtesh Hatira, top Quenstedtoceras s. str., supporting its relations Zohar Formation. PI. 6, figs. 7-9. to the cardioceratids with a questionable DERIVATION OF NAME: Type locality: Makhtesh identitfication with Prorsiceras. Hatira. MATERIAL AND OCCURRENCE: Holotype (Type STRATIGRAPHIC LEVEL: Upper Callovian. No. 1210) M-6089, specimens M-5400, 5384, 5451

GSI Bull. 76, 1983 33 U. CALLOVIAN AMMONITES Z. LEWY

(coll. M. Goldberg and M. R aab), Makhtesh DESCRIPTION: A poorly preserved fragment of a Hatira, uppermost part of the Zohar Formation. ventral part of the whorl, with coarse, widely spaced lateral ribs, bearing a ventrolateral tubercle (dorsal part damaged). Ventral short, prorsiradiate ribs become stronger in the form of Family REINECKEIIDAE Hyatt, 1900 bullae and terminate before the siphonal region, Genus REINECKEITES Buckman, 1924 where they form a shallow groove. The ventral Type species: Reineckeites duplex Buckman, 1924 ribs do not furcate from the ventrolateral tubercles. Reineckeites sp. cf. R. douvillei Stein mann PI. 7, figs. 8-10 DISCUSSION: Our fragment has the ornament pattern of the adult stage of Collotites (= cf. 1932 Reineckeia stuebeli Steinmann, var. Collotia) odysseus Mayer-Eymar (Jeannet, PI. 67) douvillei Steinmann, Corroy, p. 121; PI. 14, fig. 4, which has a high whorl section. Collotia aff. non 3, 5-6. angusttlobata (Brasil, in Spath, 1928, PI. 33, fig. c f. 1951 Reineckeites douvillei Steinm. sp., 10) also has a similar coarse ornament and a Jeannet, p. 141; PI. 49, fig. 7; PI. 57, fig. 1. broad whorl section. However, due to the c f. 1968 Reineckeites douvillei Steinmann, fragmentary nature of our specimen, no specific Bourquin, p. 54; PI. I, 2-5; PI. IV, 2; PI. X, 2; PI. 5, identification is possible. figs. 1-4. AGE: Collotia ranges from the Middle into the DESCRIPTION: A small fragment of the whorl of Upper Callovian Athleta-Zone and has been a planulate conch. The subparallel flanks are recorded as relatively rare from the Upper ornamented by irregularly spaced primary, simple Callovian Lamberti-Zone (Arkell, 1939; Callomon or bifurcating ribs. The secondaries tend to and Sykes in Duff, 1980). approach and join some of the primaries but weaken and disappear just before converging. All MATERIAL AND OCCURRENCE: (Type No. 1377) ribs are prorsiradiate, especially near the venter, M-7746 (coll. Z. Lewy), Gebel Maghara (G. Hamir, where they become stronger on the ventrolateral coord. 9838/0102), top Zohar Formation. shoulder. They weaken suddenly on the venter leaving a siphonal furrow.

DISCUSSION: The small fragment exhibits the characteristics of Reineckeites, similar in nature to the compressed R. douvillei Steinmann, with the irregularly spaced, ribbing (not the regular Family PERISPHINCTIDAE Steinmann, 1890 bifurcating pattern in Corroy, 1932; PI. 14, figs. Subfamily PROPLANULITINAE Buckman, 1921 i 3, 5-6). This species was recorded from the Genus KINKELINICERAS Buckman, 1921 i Middle (?) and Upper Callovian. However, the present small fragment does not enable Type species: Proplanulites Idnkelini Dacqu^, 1910 i undoubtable specific identification. Kinkeliniceras sp. cf. K. Idnkelini (Dacqu^) AGE: • R. douvillei is recorded from the Middle PI. 6, figs. 3, 4 Callovian and the Upper Callovian Athleta-Zone of cf. 1931 Kinkeliniceras klnkelini (Dacqu^), Spath, Switzerland (Jeannet, 1951, p. 141). p. 307; PI. 62, fig. 7. MATERIAL AND OCCURRENCE: (Type No. 1365) cf. 1958 Obtusicostites devi Spath, Collignon, PL M-5371(2) (coll. Z. Lewy), Makhtesh Hatira, 31, fig. 144. Upper Zohar Formation (middle Tsia Member). DESCRIPTION: Moderately evolute (U/D = 0.36), planulate conch. Whorl section trapezoidal with the maximum width at the umbilical shoulder Genus COLLOTIA de Grossouvre, 1917 and a slightly, narrow, rounded venter. W/H decreases with growth, especially in the young Type species: Ammonites fraasi Oppel, 1957 stage, forming the planulate coiling pattern. The Collotia sp. umbilical w all is quite steep with rounded PI. 7, figs. 11, .12 shoulders.

34 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

MEASUREMENTS: Subfamily PSEUDOPERISPHINCTINAE Schindewolf, 1925 D H W W/H U Genus GROSSOUVRIA Siemiradzki, 1898

M-7671 - 11.5 18.3 1.6 - Type species: perisphinctes subttlis, 1870 « - 18.5 18.0 0.96 - II Grossouvria sp. 49 1 9 .5 (0 .4 0 ) 1 9 .0 (0 .3 9 ) 0.97 17.51 PI. 7, fig. 15

DISCUSSION: The fragmentary single specimen forms a quarter of a volution. It differs from the The young stage has a short, prominent two Grossouvria sp. from Saudi Arabia (Imlay, umbilicolateral ribs resembling bullae, which 1970, p. D14; PI. 3, figs. 1-4) by its strongly bifurcate into prorsiradiate ribs. With growth, a prorsiradiate (not falcoid) primary ribs, all shorter secondary rib appears in between the bifurcating at the ventrolateral margins and by its pair of primaries, weakening dorsally in the higher than wide whorl section. Grossouvria sp. of middle of the flank. All ribs strengthen Spath (in Hudson, 1958; British Museum No. ventrally, become very prominent on the e71701) has alternating simple and bifurcating ventrolateral shoulder and weaken on the siphonal radiating ribs and may be close (or identical to region, resembling somewhat Proplanulites, which our "Perisphinctes" sp. has a smooth band on the siphonal region. Generally, the ribs cross the venter with a gentle MATERIAL AND OCCURRENCE: (Type No. 1368) adorally convex curvature. The sutures are not M-7815 (coll. M. Goldberg and M. Raab), Makhtesh preserved. Hatira, base Be'er Sheva Formation.

DISCUSSION: Our single specimen is poorly preserved. However, its mode of coiling and ornament is that o f the Planulitinae, among Subfamily PERISPHINCTINAE Steinmann, 1890 which it most resembles Ktnkeltniceras kihkelini "Perisphinctes? (s.l.) sp. (Dacqu^) of Spath (1931, PI. 62, fig. 7) from the PI. 7, figs. 23, 24 Upper Callovian (Athleta beds) of Cutch. Obtustcostites devt Spath, from the Upper ? 1958 Grossouvria sp., Hudson, p. 420. Callovian of Madagascar (Collignon, 1958), DESCRIPTION: Evolutely coiled, planulate, resembles our specimen in mode of ribbing. This quadrangular whorl section higher than wide (W/H Madagascan specimen is larger than our one and = 7.5/8.6 = 0.87). Flanks flattened and shows a more advanced growth stage than subparallel, rounded umbilical shoulder and an obtained by our specimen. Therefore, an almost tabulate to slightly rounded venter. Fine, undoubtable identity could not be established. sharp ribs radiate from the umbilical seam, pass Arkell (1957, p. L317) noticed the great similarity over the umbilical wall onto the flanks. Most ribs of some Obtustcostites species to those of bifurcate at the middle of the flanks from Kirikelintceras, both genera attributed by him to where they tend to bend forward, crossing the the Middle Callovian. However, the Late Callovian venter with a gentle adorally convex curvature. age of the two above mentioned species of Ribbing is very fine and dense on the young Ktnkeltniceras and Obtustcostites and the Upper volutions and coarsens gradually with growth. No Callovian Kinkeltntceras oppelt Kanjilal and Singh constrictions are discernible. The suture is only (1980) from Cutch, suggest an extension of the generally represented by the surface of a septum range of these genera into the Upper Callovian. showing a large first lateral saddle, a narrow first AGE: Our specimen is compared to Upper lateral lobe at the middle of the flank, and Callovian (Athleta-Zone) forms although the typical three, small gradually decreasing umbilical K. ktnkelint (Dacqu^) is a Middle Callovian saddles. taxon. DISCUSSION: Our fragment is similar to the MATERIAL AND OCCURRENCE: (Type No. 1223) Oxfordian Perisphinctes s. str., differing only by M-7671 (coll. M. Goldberg and M. Raab), Makhtesh the rather low point of rib-bifurcation in our Hatira, Upper Zohar Formation (middle Tsia specimen (thereby differing from Member). Dichotomospihinctes and Dichotomoceras and from

GSI Bull. 76, 1983 35 U. CALLOVIAN AMMONITES Z. LEWY the constricted Orthosphinctes). A great variety Alligaticeras sp. cf. A. raguini of Callovian perisphinctids was attributed to the (Gerard and Contaut) genus Grossouvria, perhaps to avoid the extension PI. 7, fig. 22; PI. 8, figs. 1, 2 of the ranges of well-known Oxfordian genera or cf. 1936 Orionoides raguini Gerard and Contaut, the establishment of new ones. p. 60; PI. 12, fig. la,b.

MATERIAL AND OCCURRENCE: (Type No. 1369) DESCRIPTION: Evolutely coiled planulate conch. HU-17780 (coll. L. Picard) and M-6062 (coll. M. Goldberg and M. Raab), Makhtesh Hatira. MEASUREMENTS:

HU-17880 is attributed to the Eligmus-Grossouvria D H W W/H U unit o f Hudson (1958), from the middle part of M-7745:1 100.0 25.8(0.26) 24.2(0.24) 0.93 54.0(0.54) the unit yielding M-6062 (Upper Zohar Formation). M-7852:1 139.0 35.3(0.25) 32.0(0.23) 0.91 76.0(0.55)

Genus SUBGROSSOUVRIA spath, 1924 The ornament consists of prorsiradiate ribs, Type species: Perisphinctes aberrans Waagen, 1875 being fine and densely spaced in the young stage, Subgrossouvria sp. becoming gradually more widely spaced with PI. 7, figs. 13, 14 growth. Near the venter, they bi- or trifurcate into narrower and weaker ribs, crossing the venter D ESCR IPTIO N: Evolutely coiled, whorl section with an adapical (convex) flexure. Two or three w id er than high (W/H = 15.3/12.0 = 1.27; constrictions per volution occur throughout 26.4/23.5 = 1.12) with rounded flanks and venter. ontogeny. Sutures not preserved. The young stage is ornamented with fine and dense prorsiradiate ribs which bifurcate DISCUSSION: Our evolute, planulate specimens ventrolaterally into finer ribs than the primaries are characterized by a gradual coarsening of and cross the venter with an adorally convex ornament of mainly bifurcating ribs with curvature. Ornament coarsens with growth, occasionally trifurcating ones. Several fragments becoming more widely spaced but keeping the show slight variations in W/H ratios and ribbing regular dichotomous pattern. The primary ribs may density, but the specific significance of these be radiate or slightly rursiradiate on the flanks, variations is yet unknown due to the poor state turning stronger forwards ventrolaterally. No of preservation. The two most complete specimens constrictions occur on the fragments. Sutures are resemble A. raguini in mode of ornament, not preserved. slightly differing from the French specimen which has a narrower whorl section (W/H = 0.86) and DISCUSSION: The broad rounded whorl section larger umbilicus (0.58). However, these small and the regular ornament pattern are those of morphological differences from the French Subgrossouvria. Although all three fragments holotype may merely represent its intraspecific represent different ontogenetic stages, they are variations. Other species of Gerard and Contaut assumed to belong to the same species. Most of (1936), such as A. cayeuxi and A. piveteaui have the Subgrossouvria species from Cutch (Spath, widely spaced ribs at the early ontogenetic stage 1928) have constrictions or coarser and more in contrast to the fine and dense ribs in our numerous ventral ribs. The constricted m aterial. Although our specimens are closely Subgrossouvria^) sp. (Spath, 1928, PI. 68, fig. 1) related to A. raguini, an undoubtable identity is most similar to our material, which cannot be could not be proven. Our specimens are quite undoubtably identified due to its fragmentary large for typical Alligaticeras, but no more nature. suitable taxon was found in the literature. MATERIAL AND OCCURRENCE: (Type No. 1380) AG E: A. raguini originates from the Upper M-7745(2), 7746 (coll. Z. Lewy), Gebel Maghara Callovian Athleta-Zone (Gerard and Contaut, region (Gebel Hamir), top Zohar Formation. 1936).

MATERIAL AND OCCURRENCE: (Type No. 1389) M-7745(4) (coll. Z. Lewy), Gebel Maghara, top Genus ALLIGATICERAS Buckman, 1923 Zohar Formation; M-7621 unit 5, 7852 unit '7 Type species: Ammonites alligatus Leckenby,1859 (coll. Z. Lewy), Gebel El-Minshera.

36 GSI Bull. 76, 1983 u. CALLOVIAN AMMONITES Z. LEWY

Family ASPIDOCERATIDAE Zittel, 1895 and the ventral ones weaken considerably. These Subfamily PELTOCERATINAE Spath, 1924 latter ribs form an irregularly spaced pattern due Genus PELTOCERAS Waagen, 1871 to variations in the number of ribs furcating Type species: Am. athleta Phillips, 1829 from the tubercles and the occurrence of intercalatory ventral ribs not connected to any Peltoceras trifidum (Quenstedt) tubercle. PI. 7, figs. 16-21 The suture is characterized by a very narrow asymmetric first lateral lobe (PI. 7, fig. 16). 1931 Peltoceras trifidum (Quenstedt), spath, p. 562; PI. 110, fig. 5. DISCUSSION: Peltoceras trifidum is quite similar 1951 Peltoceras trifidum Q. sp., Jeannet, p. 167; to P. athleta Phillips in mode of coiling and PI. 72, fig. 4; PI. 73, figs. 1-4; text-figs. ornament. The only feature which may 394-396. differentiate between them is the very long and cf. 1959 Peltoceras trifidum Q., collignon, PI. narrow asymmetric first lateral lobe in trifidum. 36, fig. 192. P. trifidum of Collignon (1959) loses its ribs on 1975 Peltoceras trifidum (Quenstedt), Gill and the flanks and venter at earlier stages than our Tintant, p. 102. material. It does not show the sutures well and thus may only be compared to our specimens. Gill DESCRIPTION: A complete, young specimen and Tintant (1975) recorded from the Makhtesh (M-5451, PI. 7, figs. 19-21; D = 35 mm) and two Hatira P. aff. antiquum (L6czy) in addition to P. fragmentary ones (M-6046, 7664) from a narrow trifidum, which is the only species identified stratigraphic interval at Makhtesh Hatira and two within the framework of this study. corroded fragments from Gebel El-Minshera, northern Sinai (M-7663); all are regarded as of AGE: P. trifidum is known from the Middle (?) the same species although minor variations do and mainly from the Athleta-Zone of the Upper occur, perhaps because of the various ontogentic Callovian of Switzerland (Jeannet, 1951, p. 169) stages, as well as their state of preservation. and the Upper Callovian Lamberti-Zone of Evolute, sub-quadrate whorl section with the width Madagascar (Collignon, 1959, PI. 36, fig. 1). greater than the height up to a diameter of 5 MATERIAL AND OCCURRENCE: (Type No. 1224) cm. The maximum width is at the umbilicolateral M-5451, 6046(2), 7664 (coll. M. Goldberg and M. margins even in between the tubercles. Each Raab; F. Hirsch) Makhtesh Hatira, Upper Zohar whorl section is almost twice as high and wide as Formation (Tsia Member; some of the specimens that of the preceding one. The umbilical wall o f G ill and Tintant were collected also at the rounded. base of the Be'er Sheva Formation). M-7663(2) MEASUREMENTS: (coll. Y. Druckman) Gebel El-Minshera, Upper D H W W/H U Zohar Formation, unit 6.

M-5451 Z5.6 8.5(0.33) 10.1(0.39) 1.18 1.7(0.45)

M-7664 - 17.0 18.0 1.06 Subgenus RURSICERAS Buckman, 1919 * - 19.3 18.8 0.97 Type species: Am. reversus Leckenby, 1859 The young stage has fine, densely-spaced, radiate ribs which bifurcate at the ventrolateral REMARKS: Callomon (1981, pers. comm.) regards margins and form loops on the venter. With Rursiceras as the microconch of its dimorph growth (D > 16 mm) the ribs become coarser and Peltoceras, so that Rursiceras should be assigned more widely spaced, mainly on the flanks. They at least as a subgenus of Peltoceras. develop umbilicolateral rounded projections which A small fragment from Gebel Maghara and a in later stages, when the ribs weaken on the diagenetically compressed badly preserved flanks, form the umbilicolateral bullate tubercles. specimen from Makhtesh Hatira show rursiradiate Spinose ventrolateral tubercles start to appear at ribbing characterizing Rursiceras. Their poor several ventrolateral bifurcation points, developing state of preservation hinders any attempt at a with growth into a regular pattern. The tubercles specific identification as well as preventing which evolved as dorsolateral projections comparison between them, so that meanwhile superimposed on the ribs become with growth the they are described herein as separate dominant feature, while the lateral ribs disappear undeterminable species.

GSI Bull. 76, 1983 37 Z. LEWY U. CALLOVIAN AMMONITES

give it a broader appearance and a trapezoidal Rursiceras sp. A. whorl section due to the more protruding PI. 6, figs. 5, 6 umbilicolateral ones. The venter and the flanks DESCRIPTION: A poorly preserved specimen, in between the tubercles form an almost circular evolutely coiled, planulate (partly diagenetically section, truncated dorsally by the strongly rounded compressed; W/H = 66/125 = 0.53) attaining a umbilical shoulder and the gently concave dorsum diameter of 38 mm. The last volution is (PI. 8, fig. 4). The fragment of the adult conch ornamented by slightly falcoid, rursiradiate to has very low ribs connecting between the pair of radiate ribs, which bifurcate at the middle of lateral tubercles. The ribs weaken and tend to the flank and become strongly rursiradiate towards disappear near the ventrolateral tubercle. The the venter, crossing it without weakening. Ribbing venter is almost smooth except for low rib-like coarsens and becomes more widely spaced with undulations, some connecting between the pairs growth. Sutures not preserved. of the ventrolateral tubercles. The poorly preserved sutures show a narrow bifid external MATERIAL AND OCCURRENCE: (Type No. 1307) lobe, a broad bifid first lateral saddle and a M-6065 (coll. M. Goldberg and M. Raab), Makhtesh smaller similar second lateral one, reaching the Hatira, Upper Zohar Formation (middle Tsia um bilical shoulder. The narrow and deep first Member). lateral lobe lies in the middle of the flank and is as long as the external lobe.

Rursiceras sp. B DISCUSSION: Douvill^ (1916) attributed the PL 8, fig. 3 specimens from Gebel Maghara to E. babeanus (d'Orbigny) on the basis of the broad whorl DESCRIPTION: A small fragment of an evolutely section and the horn-like pair of lateral tubercles coiled planulate conch, subparallel flanks and a of the young ontogenetic stage. However, rounded venter (W/H = 17.4/18.3 = 0.95). A slight according to the drawings in d'Orbigny (1847, PI. increase in width and height marks the adoral 181, fig. 1), the ventrolateral tubercles weaken direction on which the generic identification is and disappear at a diameter over 85 mm, thus based. Strong, sharp rursiradiate primaries differin g from the coarsely tuberculated large bifurcate at the middle of the flanks into sharp, fragment from Sinai (PL 8, figs. 4-6). Two species strongly rursiradiate ribs which cross the venter. described by Jeannet (1951) resemble our Sutures not preserved. fragments: E. spinigerum Rollier and E. MATERIAL AND OCCURRENCE: (Type No. ferrugineum Jeannet. The refigured holotype of E. 1445), M-7746 (coll. Z. Lewy), Gebel Maghara spinigerum shows morphological similarity with E. region (G. Hamir), top Zohar Formation. ferrugineum. This latter species is represented by several specimens (e.g., var. A) of a broad variability in whorl height (H/D = 0.32-0.29), Genus EUASPIDOCERAS Spath, 1931 width (W/D = 0.42-0.31) and umbilical ratio- (U/D = 0.50-0.46) which include the pattern of the Type species: Ammonites perarmatus J. Sowerby, holotype of E. spinigerum Rollier. E. ferrugineum 1882 occurs in Switzerland from the lower Euaspidoceras ferrugtneum Jeannet Athleta-Zone to the lower Lamberti-Zone, whereas PI. 8, figs. 4-6 the single specimen of Rollier is known from the upper Athleta-Zone. It seems that Jeannet (1951) 1916 Aspidoceras babeaui d'Orbigny, Douvill^, p. assigned to his species ferrugineum a broad, 70; PI. 8, fig. 6a,b. morphological and stratigraphical range which 1951 Euaspidoceras ferrugineum Jeannet, p. 202; may include E. spinigerum Rollier. Therefore, here PI. 92, fig. 1; PI. 93, fig. 1. it is preferred to attribute the material from ?1951 Euaspidoceras spinigerum Rollier, Jeannet, Sinai to E. ferrugineum, although it may be a p. 205; PL 94, fig. 3, text-fig. 484. junior synonym of E. spinigerum Rollier.

DESCRIPTION: Moderately large, evolute coiling AGE: Aspidoceratinae appear in Europe from the with a wide whorl section (W/H = 47/42 = 1.12 in Upper Callovian Lamberti-Zone (Callomon, 1981, between the ribs). The widely-spaced, strong pers. comm.); E. ferrugineum occurs in Switzerland umbilicolateral and ventrolateral horny tubercles in the Athleta-Zone and base Lamberti-Zone of

38 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY the Upper Callovian (Jeannet, 1951). DISCUSSION: Our fragmentary specimens have horn-like ventrolateral widely spaced tubercles, MATERIAL AND OCCURRENCE: M-7745(3) (coll. resembling the ornament of Paraspidoceras from Z. Lewy), Gebel Maghara, top Zohar Formation. the Upper Oxfordian. Usually, Paraspidoceras ( =Extranodites Jeannet, 1951) has rather long and narrow horny tubercles from the young Subfamily ASPIDOCERATINAE Zittel, 1895 ontogenetic stages, tending to depressed sections Genus PARASPIDOCERAS Spath, 1925 with clavate horns. Our specimens are adult Type species: Am. mertani Oppel, 1863 stages which bear broad, coarse, horn-like short tubercles resembling the ventrolateral row of some " Paraspidocerasf, sp. Euaspidoceras, but lack the dorsolateral tubercles. Fig. 6E Better material is needed to decide whether it 1975 Paraspidoceras sp. nov., Gill and Tintant, p. is a new form. Gill and Tintant (1975) have recorded from 103. the same locality and stratigraphic level DESCRIPTION: Evolutely coiled, large conchs. Paraspidoceras sp. nov. Although not described or The whorl section of the adult fragment in figured, it is reasonable to assume that it is between the tubercles is circular, whereas the identical to our material. In the absence of any robust ventrolateral tubercles give it a ventral ribbing on our fragment, no relations trapezoidal (or even triangular) shape (Fig. 6E). could be established with Peltoceras (?) antiquum The reconstruction of the conch according to the (L6czy, 1915, PI. 26, figs. 1-2). fragments shows a broad, slightly rounded, smooth MATERIAL AND OCCURRENCE: M-6149(2), venter and rounded flanks in between the 6025(7) (coll. M. Goldberg and M. Raab; Z. Lewy), tubercles. The prominent horn-like triangular Makhtesh Hatira, lower part of Be'er Sheva ventrolateral tubercles may stretch dorsally as Formation, attributed to the Late Callovian on pseudo-ribs mainly in whorls up to 4 cm in the basis of its association with Pachyerymnoceras height, whereas in H > 5 cm, they weaken and levantinense Lewy nov. sp. (Type No. 1306). disappear ventrally to the middle of the flank. No ribs or dorsolateral tubercles occur. Sutures only partly preserved.

*

ACKNOWLEDGEMENTS L. Buchbinder, B.H. Conway, A. Ehrlich, H. Frenkel, F. Hirsch, S. Moshkovitz, A. Parnes and especially M. Goldberg (Geological Survey of This study is based mainly on ammonites Israel), J. Thierry (University of Dijon, France) collected at Makhtesh Hatira (Kurnub anticline), and J.H. Callomon (University College, London) Israel, by M. Goldberg and M. Raab. A few contributed to this study through discussions, additional specimens were found by L. Picard, F. criticism and data from their own work on the Hirsch and the author. The specimens from Gebel Jurassic stratigraphy. Maghara and Gebel El-Minshera (northern Sinai) R. Imlay (Smithonian Institution, Washington were collected mainly by the author and some D .C.) sent me the photos of an ammonite from specimens by Y. Bartov, Y. Druckman and the Saudi Arabia, described by him in 1970, with the late R. Freund. kind permission to refigure it. The lithostratigraphy of the Jurassic Great technical assistance has been offered sequences in the Negev, Israel, northern Sinai and by C. Alafi, R. Bogoch, M. Dvoracheck, B. Katz, Mount Hermon has been worked out by M. R. Knafo, S. Levy, Y. Levy, A. Pe'er and N. Goldberg and used herein with his kind Shragai. To all of them the author is greatly permission. indebted.

39 GSI Bull. 76, 1983 Z. LEWY U. CALLOVIAN AMMONITES

REFERENCES BANDEL, K., 1981. New stratigraphical and structural evidence for lateral dislocation in the Jordan Rift Valley ABDALLAH, A.M., EL ADINDANI, A. connected with a description of the and FAHMY, N., 1965. Stratigraphy Jurassic rock column in Jordan. of the Lower Mesozoic rocks western Neuer Jahrb. Geol. Palaontol., Abh. side of Gulf of Suez, Egypt. 161, pp. 271-308, 12 figs. U.A.R. Geol. Surv. Paper 27, 23 p., BASHA, S.H., 1980. Ostracoda from the 7 figs., 1 pi. Jurassic system of Jordan. Including AL-FAR, D.M., 1966. Geology and coal a stratigraphical outline. Rev. Espan. deposits o f G ebel El-M aghara (northern Micropaleontol., Vol. 12, . pp. 234-254, Sinai). U.A.R. Geol. Surv., Paper 37, 4 pis., 3 figs. 59 p., maps. BARZEL, A. and FRIEDMAN, G.M., 1970. ARKELL, W.J., 1939. The ammonites The Zohar Formation (Jurassic) in succession at the Woodham Brick southern Israel: A model of Company's pit, Akeman Street station, shallow-water marine carbonate Buckinghamshire and its bearing on sedimentation. Isr. J. Earth-Sci., Vol. the classification of the Oxford Clay. 19, pp. 183-207, 22 figs. Geol. Soc. London, Quat. J., Vol. BENDER, F., 1974. Geology of Jordan. 95, pp. 135-222, pis. 8-11, 4 figs. Gebruder Borntraeger, Berlin, Stuttgart. ARKELL, W.J., 1952. Jurassic ammonites 196 p., 160 figs. from Jebel Tuwaiq, Central Arabia BOURQUIN, J., 1968. Les Reineck^ides. (Stratigraphical introduction by R.A. Ann. Sci. 1'Univ. Besagon, 3e S^r., Bramkamp and M. Steineke). Phil. Geol. fasc. 4, 169 p., 51 + 30 Trans. Roy. Soc. London, Vol. 236 pis. B, pp. 241-313, pis. 15-31, 11 figs. BRAMKAMP, R.A. and RAMIREZ, L.F., ARKELL, W.J., 1957. Mesozoic 1958. Geologic Map of the Northern Ammonoidea (part), in: Moore, R.C. Tuwaiq Quadrangle Kingdom o f Saudi Treatise on Invertebrate Paleontology. Arabia. U.S. Geol. Surv., Misc. P t . L . Mollusca 4, Cephalopoda, Geol. Inv. Map 1-207 A. Ammonoidea. Geol. Soc. Amer. and BUCHBINDER, L., 1979. Facies, Univ. Kansas Press, 4 90 p., 5 58 environment of deposition and figs. correlation of the Zohar (Brur ASSERETO, R., BARNARD, P.*D.W. and Calcarenite), Karmon and Shderot FANTINI SESTINI, N., 1968. Jurassic Formations in the Ashdod Area. Isr. stratigraphy of the Central Elburz Geol. Surv. Rep. OD/3/79, 45 p., (Iran). Riv. Ital. Paleont., Vol. 74, 11 pis., 6 figs. pp. 3-21, 11 tabs. AUROUZE, G., BELLON, J., BIZON, J.-J. CALLOMON, J.H., 1962. Notes on the and JO U R N ELI, G., 1956. Sur la Callovian and Oxfordian stages. Colloq. presence du genre Kilianina dans le Jurassique, Luxemburg, 1962, pp. Bassin de Paris. Soc. Geol. Fr. 269-291. Bull., Vol. 6, pp. 221-225. C ALLO M O N, J.H., 1963. Sexual AUROUZE, G. and BIZON, J.-J., 1958. dimorphism in Jurassic ammonites. Rapports et differences des deux Trans. Leicester Lit. Phil. Soc., Vol. genres de Foraminiferes: Kilianina 57, pp. 21-56, 1 pi., 9 text-figs. (Pfender) et Meyendorffina n. gen. CHARPY, N. and THIERRY, J., 1977. Rev. Micropaleontol., Vol. 1, pp. Dimorphisme et polymorphisme chez 67-74. Pachyceras Bayle (Ammonitina,

40 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

Stephanocerataeeae) du Callovien d'apres les explorations de M. sup^rieur (Jurassique moyen). Haliotis, Couyat-Barthoux. Paleontologie. Mem. Vol. 6, pp. 185-218, 5 pis., 6 figs. Acad. Sci., 54, 2me Ser., 184 p., COATES, J., GOTTESMAN, E., JACOBS, 21 pis., 50 figs. M. and ROSENBERG, E., 1963. Gas D O UVILL^, R., 1912. Etudes sur les discoveries in the western Dead Sea Cardioc^ratides de dives, Villers-sur-Mer region. 6th World Petrol. Cong., e t quelques autres gisements. Soc. Frankfurt/Main, Germany, Sect. 1, G^ol. Fr., M^m. Paldont., T.19, n. Paper 26, pp. 21-36. 45, 77 p., 5 pis., 84 figs. COLLIGNON, M., 1958. Atlas des fossiles DUBERTRET, L., 1955. Carte G^ologique caract^ristiques de Madagascar. Fasc. d u Liban au 1:200,000 with 2 (Bathonien Callovien). Serv. G^ol. explanatory notes, Rep. Liban. Min. Tananarive, pls.^6-33. Trav. Pub., Beyrouth. 74 p., 8 pis., COLLIGNON, M., 1959. Atlas des fossiles 30 figs. caract^ristiques de Madagascar. Fasc. DUBERTRET, L., 1963. Liban, Syrie: 3 (Oxfordien) Serv. G^ol. Tananarive, Chatne des grands massifs cotiers et pis. 34-46. confins a l'Est. In: Dubertret, L. CORROY, G., 1932. Le Callovien de la Lexique stratigraphique International, bordure orientale du Bassin de Paris. Asie, Fasc. 10 cl, pp. 1-155, M^m. expl. carte g^ol. Fr. 337 p., C.N.R.S. DUBERTRET,L., 1966. Liban, Syrie et 29 pis., 62 figs. bordure des pays voisins. Pt. 1: COUFFON, O., 1919. Le Callovien du Tableau stratigraphique, avec carte Chalet. Angers, 245 p., 18 pis. g^ologique au millionieme. Notes et DERIN, B., 1974. The Jurassic of M^m. Moyen-Orient, Vol. 8, pp. Central and Northern Israel. Ph.D. 251-358, 35 figs., map. Thesis, Hebrew Univ. Jerusalem, 152 DUFF, K.L., 1975. Paleoecology of a p. (in Hebrew), 18 pis., 29 figs. bituminous shale - the Lower DERIN, B. and REISS, Z., 1966. Oxford Clay of central England. Jurassic microfacies of Israel. Isr. Palaeontology, Vol. 18, pp. 443-482, Inst. Petrol., Spec. Publ., 43 p., 320 19 figs. figs., 2 tabs. DUFF, K.L., 1980. Callovian correlation DERIN,B. and GERRY, E., (1972) 1975. chart (with a contribution on Jurassic b i ostratigraphy and subzones of the stage by J.H. environments of deposition in Israel. Callomon and R.M. Sykes) In: Cope, Rev. Espan. Micropaleontol., Ser 1, J.C.W. A correlation of Jurassic Proc. 5th African Micropal. Colloq., rocks in the British Isles. Pt. 2: Addis Ababa (Ethiopia), pp. 175-198, Middle and Upper Jurassic. Geol. Soc. 4 figs. London, Spec. Rep. 15, pp. 45-48, DONOVAN, D.T., CALLOMON, J.H. and fig. 8. HOWARTH, M.K., 1981. Classification DUNNINGTON, H.V., WETZEL, R. and o f th e Jurassic Ammonitina, in: MORTON, D.M., 1959. Mesozoic and House, M.R. and Senior, J.R: The Paleozoic, in: Lexique stratigraphique Ammonoidea, pp. 101-155. Systematic International, Asie, Fasc. 10a, Iraq, Association Special vol. 18, London C.N.R.S., 333 p., 6 pis.. and New York, Academic Press. FARAG, I. and SHATA, A., 1954. DOUVILL^, H., 1916. Les terrains Detailed geological survey of secondaires dans le Massif du El-Minshera Area. Bull. Inst. Desert Moghara a l'est de l'Isthme de Suez, d'Egypte, IV, pp. 5-82, 8 pis.

GSI Bull. 76, 1983 41 Z. LEWY U. CALLOVIAN AMMONITES

FARAG, I. and OMARA, S., 1955. On Proc. Isr. Geol. Soc. 1963-4, in the occurrence of marine Middle Isr. J. E arth -Sci., Vol. 13, pp. Jurassic deposits at Gebel El-Minshera 169-172, 2 figs. (Northern Sinai, Egypt). Bull. Inst. GOLDBERG, M., 1 9 6 7 . Supratidal Desert d'Egypte, Vol. 1, pp. dolomitization and dedolomitization in 165-178, 3 figs., 4 phot. Jurassic rocks of Hamakhtesh Haqatan, FREBOLD, H. and TIPPER, H.W., 1975. Israel. J. Sed. Petrol., Vol. 37, pp. Upper Callovian and Lower Oxfordian 760-773, figs. 1-22. ammonites from southeastern Bowser GOLDBERG, M., 1969. The Jurassic of Basin, British Columbia. Can. J. Majdal Shams area, Mt. Hermon. Earth-Sci., Vol. 12, pp. 145-157, 2 Isr. Geol. Surv. 1 section. pis., 2 figs. GOLDBERG, M., 1970. The FRENKEL, H., 1975. Pseudocyclammina lithostratigraphy of Arad Group (? ), P. smouti Banner, from the (Jurassic) in the northern Negev. Bathonian Sherif Fm. of Gebel Unpub. Ph.D. Thesis, Hebrew. Univ. Maghara (Northern Sinai). Isr. J. Jerusalem, 137 p. 28 figs. (in Earth-Sci., Vol. 24, pp. 49-52, 9 figs. Hebrew). FURRER, U. and SEPT FONTAINE, M., GOLDBERG, M., BARZEL, A., COOK, P. 1977. Nouvelles donnees and MIMRAN, Y., 1971. Preliminary biostratigraphique (& l'aide des columnar section of the Jurassic of Foram iniferes) dans le Dogger k Gebel Maghara. Isr. Geol. Surv. Rep. facifes br iangonnaise des Pr^alpes MM/1/71. m^dianes romandes (Suisse). Eclogae GOLDBERG, M. and FRIEDMAN, G.M., Geol. Helv., Vol. 70, pp. 717-737, 2 1 9 7 4 . Pa 1 e o e n v i r o n m e n t s and figs., 2 pis. paleogeographic evolution of the GERARD, Ch. and CONTAUT, H., 1936. Jurassic System in Southern Israel. L es ammonites de la zone a Isr. Geol. Surv. Bull. 61, 44 p., 8 Peltoceras athleta du centreouest de pis., 16 figs. la France. Soc. Ge'ol. Fr. M^m., GOLDBERG, M. and BOGOCH, R., 1978. n.s., T. 13, n. 29, 79 p., 19 pis., Dolomitization and hydrothermal 18 text-figs. mineralization in the Brur Calcarenite GILL, D., 1966. Petrographic study of (Jurassic), southern Coastal Plain, some carbonate rocks from Jurassic Israel. Isr. J. Earth-Sci., Vol. 27, outcrops in Makhtesh Qatan, Southern pp. 36-41, 11 figs. Israel. Isr. J. Earth-Sci., Vol. 14, HAAS, O., 1 95 5. Revision of the pp. 122-138, 8 figs. Jurassic ammonite fauna of Mount GILL, G. A. and TIN TAN T, H., 1975. Hermon, Syria. Am. Mus. Nat. Hist. Les ammonites calloviennes du Sud Bull., Vol. 108, 210 p., 30 pis., 4 d'Israel. Stratigraphie et relations text-figs. pal^ogtfographiques. C .R . somm. Soc. HIRSCH, F., 1976. Sur 1'origine des g^ol. Fr., 1975 au Soc. Ge'ol. Fr. particularismes de la fauna du Trias Bull., Vol. 17, pp. 103-106, 2 figs. et du Jurassique de la plate-forme GOLDBERG, M., 1963. Reference section africano-arabe. Soc. G^ol. Fr. Bull., o f Jurassic sequence exposed in Vol. XVni, pp. 543-552, 3 figs. Hamakhtesh Hagadol (Kurnub anticline). HIRSCH, F., 1980. Jurassic Bivalves and Isr. Geol. Surv. Location map and Gastropods from Northern Sinai and section. Southern Israel. Isr. J. Earth-Sci., GOLDBERG, M., 1964. Problems of Vol. 28, pp. 128-163, 5 figs, 13 Jurassic stratigraphy in southern Israel. pis.

42 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

HUDSON, R.G.S., 1 958. The Upper LOMINADZE, T.A., 1 97 5. Callovian Jurassic faunas of Southern Israel. Hectioceratinae from the northern Geol. Mag., Vol. 95, pp. 415-425, 1 Caucasus. Akad. Nauk. Gruzia CCP., fig- Inst. Paleont. 1975, 98 p., 9 pis., IMLAY, R.W., 1 97 0. Some Jurassic 43 figs. (in Russian). ammonites from Central Saudi MAYNC, W., 1966. Microbiostratigraphy of Arabia. U.S. Geol. Surv. Prof. Paper the Jurassic of Israel. Isr. Geol. 643-D, 17 p., 4 pis., 3 figs. Surv. Bull. 40, 56 p., 15 pis. JEANNET, A., 1951. Stratigraphie und MEDD, A.W., 1982. Nannofossil zonation P a 1 a o n t o 1 o g i e des oolitischen o f the English Middle and Upper Eisenerzlagers von Herznach und Jurassic. Marine Micropaleontol., Vol. seiner Umgebung. T. 1. Beitr. Geol. 7, pp. 73-95, 4 figs. Schweiz, Geotech. Ser. 13, 240 p., MOSHKOVITZ, S. and EHRLICH, A., 107 pis., 545 figs. 1976. Distribution of Middle and KANJILAL, S. and SINGH, C .S .P ., 1980. Upper Jurassic calcareous nannofossils A n ew ammonoid species of in the northeastern Negev, Israel Kinkeliniceras with Hubertoceras-like and in Gebel Maghara, northern Sinai. inner whorls from Jurassic rocks of Isr. Geol. Surv. Bull. 69, 47 p., Habo Hill, District Kutch (Gujarat), 29 figs., 8 pis. W. India. J. Moll. Stud., Vol. 46, MOSHKOVITZ, S. and EHRLICH, A., pp. 224-226, 1 fig. 1981. Late Jurassic calcareous KATZ, A., 1968. Petrological and nannofossils in Israel's offshore and geochemical problem s in the Mahmal on land areas. Isr. Geol. Surv. Formation. Makhtesh Ramon (Southern Current Res., 1980, pp. 65-72, 5 figs. Israel). Unpub. Ph.D. Thesis, Hebrew NEVO, E., 1963. The Jurassic strata of Univ. Jerusalem, 173 p., figs., 2 Makhtesh Ramon, Isr. Geol. Soc., tabs, (in Hebrew). February, 1963, 11-12, section. KIER, P.M., 1972. Tertiary and Mesozoic NOETLING, F., 1887. Der Jura am Echinoids of Saudi Arabia. Smithson. Hermon. Eine g e o g n o s t i s c h e Contrib. Paleobiol. 10, 242 p ., 67 Monographie. Stuttgart, E. pis., 50 figs. Schweizerbartisch Vlg., 46 p., 7 pis. LEWY, Z., 1981. Callovian (Mid-Jurassic) ORBIGNY, d'f A., 1842-1891. Pal^ontologie stratigraphy of the Middle East. Isr. Frangaise, Terrains Oolitiques ou Geol. Surv. Current Res. 1980, pp. Jurassiques; C^phalopodes. Paris, 642 42-43, 1 fig. p., 234 pis. LEWY, Z., 1981a. A Late Bathonian - ORBIGNY, d', A., 1844. Pal^ontologie du Late Callovian unconformity in the voyage de M. Hommaire de Hell, Middle East. New sletters on Stratig., in: Hommaire de Hell: Les steppes Vol. 10, pp. 27-33, 1 fig. de mer Caspienne, le Caucase, la L (5 C Z Y , L. von L 6 c z j i n , 1915. Crimee et la Russie meridionale. 3. Monographie der Villanyer 4 17- p. + atlas. Paris and Callovien-Ammoniten. Geol. Hungar., Strasbourg. Vol. 1, pp. 255-502, 14 pis., 149 PALFRAMAN, D .F .B ., 1967. Variation and text-figs. ontogeny of some Oxford Clay LOMINADZE, T.A., 1970. Mid-Callovian ammonites: Distichoceras bicostatum Ery mnoceratidae from the northern (Stahl) and H arioceras baygieri Caucasus. Akad. Nauk Gruzia CCP., (D 'Orbigny), from England. Inst. Paleont., 1970, 70-97 pis., 14 Palaeontology, Vol. 10, pp. 6-94, pis. figs. (in Russian). 9-13, 11 text-figs.

GSI Bull. 76, 1983 43 U. CALLOVIAN AMMONITES Z. LEWY

PARNES, A., 1961. On the occurrence REINER, W., 1968. Callovian gastropods of Pseudopygurus Lambert in Southern from Hamakhtesh Hagadol (Southern Israel. Bull. Res. Coun. of Isr. Vol. Israel). Isr. J. Earth-Sci., Vol. 17, 10G, pp. 216-222, pi. 1, fig. 1. pp. 171-198, 3 pis., 2 figs. PARNES, A ., 1981. Biostratigraphy of the REYMENT, R.A., 1 9 7 2 . Callovian Mahmal Formation (Middle and Upper Ammonites Q a m b e r t i -Zone) found in Bajocian) in Makhtesh Ramon (N egev, an erratic concretion near Svedala, Southern Israel). Isr. Geol. Surv. Bull. Scania. Bull. Geol. Inst. Univ. 74, 55 p., 11 pis., 5 figs. Uppsala, (n.s.), Vol. 3, pp. 19-25, 5 PONIKAROV, V.P. (edit.), 1967. The pis., 1 fig. Geology of Syria. Explanatory notes on th e geological map of Syria, SAID, R., 1962. The geology of Egypt. scale 1:500,000. Pt. I. Stratigraphy, N.Y., Amsterdam, Elsevier, 377 p., 71 ill., 10 pis., 27 tabs., igneous rocks and tectonics. S.A.R. SPATH, L.F., 1927-1931. Revision o f the Dept. Min. Res., 229 p., 35 figs. POWERS, R.W., RAMIREZ, L.F., Jurassic cephalopod fauna of Kachh REDMOND, C.D. and ELBERG, E.L. (Cutch). Pts. 1-4. Palaeontologia Jr., 1966. Geology of the Arabian Indica n.s., Vol. 2, pts. 1-6, 945 p., 130 pis. Peninsula, Sedimentary geology of Saudi Arabia. U.S. Geol. Surv. Prof. THIERRY, J., 1976. Paleobiogeographie de Paper 560-D, pp. 1-147, 10 p is., quelques Stephanocerataceae (Ammonitina) 14 figs. du Jurrasique moyen et superieur; PUGIN, L., 1964. Ammonites prealpines. une confrontation avec la theorie Etude critique des Lytoceratina du mobiliste. Geobios, Vol. 9, pp. Dogger. Schweiz. Palaont. Abh. 80, 291-331, 9 figs. 67 p., 4 pis., 10 text-figs.

VAIL, P.R., MITCHUM, R.M. Jr. and THOMPSON, S., 1977. Global Cycles RANGHEARD, Y., 1961. £tude of Relative Changes of Sea-Level, in: paleontologique des representants du Payton, C.E. (edit): Seismic genre Hecticoceras du Callovien du S t r a t i g r a p h-a p p 1 i c a t i o n s to Jura Franc-comtois. Ann. Sci. Univ. hydrocarbon-exploration. Am. Assoc. Pet. Besan$on. 2me s£ r. G ^ o l., fasc. 14, GeoL Mem. 26, pp. 83-97, 7 figs. pp. 135-176, 4 pis., 15 text-figs. van HINTE, J .E ., 1976. A Jurassic time REDMOND, C.D., 1964a. The foraminiferal family Pfenderinidae in the Jurassic scale. Am. Assoc. Pet. Geol. Bull., o f Saudi Arabia. Micropaleontolcgy, Vol. 60, pp. 489-497, 4 figs. Vol. 10, pp. 251-263, pis. 1-2, 3 text-figs. WESTERMAN, G.E.G., 1965. Septal and REDMOND, C.D., 1964b. Lituolid sutural pattern in evolution and foraminifera from the Jurassic and taxonomy of Thamboceratidae and Cretaceous of Saudi Arabia. Clydoniceratidae (M. Jurassic, M icropaleontolgy, Vol. 10, pp. 405-414, Ammonitina). J. Paleontol., Vol. 39, pis. 1-2, 2 text-figs. pp. 864-874, pis. 101-102, 4 text-figs. REDMOND, C.D., 1965. Three new WIEDMANN, J., 1962. Ammonites aus der genera of foraminifera from the Vascogotischen Kreide (Nordspanien). 1. Jurassic of Saudi Arabia. P h y lloceratina, Lytoceratina. 'Micropaleontology, Vol. 11, pp. Palaeontogr. Abt. A., 118, pp. 133-140, pi. 1. 119-237, pis. 8-14, 58 figs.

GSI Bull. 76, 1983 44 U. CALLOVIAN AMMONITES Z. LEWY

WIEDMANN, J. and KULLMANN, J., ZEISS, A., 1974. Die Callovien-Ammoniten 1979. Nubidites omarai n.g. n.sp., Athiopiens und ihre zoogeographische e in neuer Ammonit aus dem Stellung. Palaeontol. Z., Vol. 48, pp. Nubischen Sandstein Agyptens. 269-282, 3 figs., pi. 37. Palaeontol. Z ., Vol. 53, pp. 248-258, 4 figs.

GSI Bull. 76, 1983 45 U. CALLOVIAN AMMONITES Z. LEWY

Figure 4. A -D , F: Pachyerymnoceras levantinense nov. sp., (type 1207); A-D : various ontogenetic stages of the same specimen, x 1, (coll. M. Goldberg and M. Raab); Es Pachyerymnoceras philbyi (Arkell), (type 1208), x 1, HU-30980, Makhtesh Hazera, Tsia Mbr., Upper Zohar Fm., (coll. E. Nevo); compare the rounded whorl section to the depressed ones of P. levantinense in Fig. 4 F; F: HU-30979, x 1, Makhtesh Hatira, lower part of Tsia Mbr.; G: Pachyceras spathi nov. sp., (type 1249), x 1, M-7691, holotype, Makhtesh Hatira, base Be'er-Sheva Fm., (coll. M. Goldberg and M. Raab).

GSI Bull. 76, 1983 46 U. CALLOVIAN AMMONITES Z. LEWY

GSI Bull. 76, 1983 47 Z. LEWY U. CALLOVIAN AMMONITES

Figure 5 A: Pachyceras lalandeanum (d'Orbigny), (type 1386), x 1, M-7745, G . Maghara, top Zohar Fm., (coll. M. Goldberg); B: Pachyceras magharense nov. sp., (type 1392), x 1, M-7745, holotype, G. Maghara, top Zohar Fm., (coll. M. Goldberg).

48 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

GSI Bull. 76, 1983 49 Z. LEWY U. CALLOVIAN AMMONITES

Figure 6 A: Pachyceras crassum R. Douville', (type 1387), x 1, M-7745, G. Maghara, top Zohar Fm., (coll. Z. Lewy); B: Pachyerymnoceras sp! c f. P. Jarryi (R. Douvill<0, (type 1380), x 1, M-7745, G. Maghara, top Zohar Fm., (coll. M. Goldberg); C: Pachyceras sp., (type 1367), x 1, M-5339, Makhtesh Hatira, middle Tsia Mbr., Upper Zohar Fm., (coll. M. Goldberg and M. R aab); D: cf. "Quenstdtoceras" sp., (type 1305), x 2, M-7261, G. El-Minshera, Upper Zohar Fm., unit 5, (coll. Z. Lewy); E: "Paraspidoceras" sp., (type 1306), x 1, M-6025, Makhtesh Hatira, lower part of Be'er-Sheva Fm., (coll. Z. Lewy); F: Levanticeras sinaiense nov. gen. and sp., (type 1206), x 1, M-7261, G. El-Minshera, Upper Zohar Fm., unit 5, (coll. Z. Lewy); G: Pachyerymnoceras levantinense nov. sp., (type 1207), x 1, M-5328, Makhtesh Hatira, upper part of Tsia Mbr., Upper Zohar Fm., (coll. M. Goldberg and M.

Raab); H: Pachyerymnoceras sp. cf. P. jaryyi (R. Douville), (type 1388), x 1, M-7745, G. Maghara, top Zohar Fm., (coll. M. Goldberg); I,J: Levanticeras levantinense nov. gen. and sp., (type 1205), Tsia Mbr., Upper Zohar Fm., (coll. Z. Lewy); I: M-7261, G. El-Minshera, x 1; J: M-7814, Makhtesh Hatira, x 6.

50 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

GSI Bull. 76, 1983 51 Z. LEWY U. CALLOVIAN AMMONITES

Chalky Lst. M arl Sandstone

Figure 7. Distribution chart of the Jurassic ammonites at .Makhtesh r, Hatira (Kurnub anticline), southern Israel (measured and sampled by M. Goldberg and M. Raab; Goldberg, 1963).

52 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES Z. LEWY

Figure 8. Distribution chart of the Jurassic ammonites at Gebel El-Minshera, northern Sinai (Israeli grid 9690/0219; measured and sampled by Z. Lewy).

GSI Bull. 76, 1983 53 M > > 9 w X m r X 3D z o H (A z 3) H m z (/> o 3 > H < 3 c < r r i « X > JO > H S s *1 > s > X > H J0 z o > z o ® m m r CD z o X i x c r z o HI HI r- HI \ fo t tvm i § o > 0 J0 X a N o > *D m > z x JO T) z H O c *0 HI CM o X d X c *n s a S3* m 31 $ N O X Ui m I > Z Z z H m O) *D m o m O) o H > X > s r Z Z m m CD >z L v m itrti M m * Cwmttvm C or* i JL to fr-. rt c 3 1 50 2 K* 8 2 td -O »- 0 8 ts l (b fr-. (b ft N H HH n 5 0 fD h to to ft n 01 o 5* c R • 1 to tr 8 S CO & £ *1 c •d 2 GSI Bull. 76, 1983 ■ h (b M a - g fr-. to H tr c a K» o a *-3 sc 1 i to I? (b c fr-. a t-3 fr-. to fr-. a rt ft) h to rt (b s l«. > ± CO fr-. ft to CO ►1 §• t* 1 J 1 CO to M. fr-. to ts §• ft t PEL) U. CALLOVIAN AMMONITES fr-t 1 CO o ? w w t-* ft 0 ? Kl to to a- fr-. to § 0B a ft -Q n 1 r r H fi) cc 0 1 fr-. o fr~> ft » rt to to S fr-. &i CO o cn fr-. ft h % *d 1 fr-. fii cn *0 tr rt to h ••si t3 to rt 0 o ge • t i \ Levanticeras levantinense LEWY nov. gen. and sp. | ng •

| Levanticeras sinaiense LEVY nov. gen. and sp. j re S fr-. c to a• tr > a ►t fi» fr-. a* i o 0 2 O' d h s ! c ■c «: *K3 < a : >«. a s to O r*2 s 3 O tt to (b <: fii a ft K< ra *0 c a i o 8 &i & •e fc 1 t ♦- S fr-. I 8 S •o ►» 50 P ft fii to CD r t r t ce 1 o 0 *1 2 & a »i c c T3 1 I to CO 3 s a 0 & <& to 8 h 0 § 0 8 2 o r t ♦i 1 1 < CO M. 3 O to to 6 & 8 5 §• •c •g 1 Ire. < * I M § fii £ tb fii a c s p o s to K. fii K< a fit 3- C ►n fii 8 < CO fii § to

1 CO to to 1 B 5 O Ui to h 0 rt »<•. N 3 o ►f lb 8 • M fi CO a 53 so 2. fr- n> & c fr-. (b fr-. fr- ► fi 0 f c fr- c r z . 1 h > 0 r t >r fr-. a *• a a to o >3 S. ft a s 2 CO 1 K- ►o •M to to c s fr-. to CO 8 O ▼ » to fr-. CO J1 a a o rt- c h 8 2 (0 (A fr-. to co c h s 2 W tJ 3 I 1 S3 § § h Di to S1 a I c fit to g. ♦1 h h c •s. S. •V 3 to 5 6 8 2 (0 2 (Q ■s c r V m X S e a l* t a s s e m b l a g e ! LO W E R c * c

i f t - —EXPOSED

Figure 9. Distribution chart of Middle Jurassic ammonites in southern Israel and northern Sinai Z. LEWY

and the recorded ranges of some of the species elsewhere. 54 U. CALLOVIAN AMMONITES Z. LEWY

Figure 10. Stratigraphic correlation of Jurassic formations between northern Sinai, southern Israel and central Saudi Arabia.

GSI Bull. 76, 1983 55 GSI Bull. 76, 1983 U. CALLOVIAN AMMONITES

Figure 11. Generalized lithostratigraphic and revised chronostratigraphic correlation Z. LEWY

of Middle to Upper Jurassic formations in southern Israel and central Saudi Arabia. 56 PLATES 1-8 EXPLANATION OF PLATE 1

Figures

1-3 Sowerbyceras tietzei (Till), (type 1378), x 1, top Zohar Fm., Up. Callovian. 1. M-7746:l strongly constricted; G.Maghara region (G. Hamir). 2-3. M-7745:l weakly constricted; G. Maghara.

4 Sowerbyceras sp., (type 1379), M-7745:l, x 1, G. Maghara, top Zohar Fm., Up. Callovian.

5 Phylloceras plicatum Neumayr, (type 1231), M-6046, x 1, Makhtesh Hatira, upper part of Tsia Mbr., Upper Zohar Fm., Up. Callovian.

6 Lunuloceras sp. cf. L. lunuloides (Kilian), (type 1366), M-7810, x 1, Makhtesh Hatira, lower part of Be'er-Sheva Fm., Up. Callovian.

7-8 Pseudobrightia sp., (type 1383), M-7745:l, x 1, G. Maghara, top Zohar Fm., Up. Callovian. 7: tricarinate venter.

9-12 Kheraites ferrugineus Spath, (type 1381), x 1, G. Maghara, top Zohar Fm., Up. Callovian. 9-10: M-7745:l; 11—12: M-7745:3 coarsely ornamented adult stage.

13-14 Lytoceras sp. cf. L. adelae (d'Orbigny), (type 1376), M-7745. x 1, G. Maghara, top Zohar Fm., Up. Callovian.

15-16 Kheraites intermedium (Spath), (type 1382), x 1, G. Maghara, top Zohar Fm., Up. Callovian. 15: M-7745:2; 16: M-7745:l, ornament weakens with growth.

17-18 Brightia sp. A, (type 1232A), M-7670, x 1, Makhtesh Hatira, upper part of Be'er-Sheva Fm., Lower (?) Oxfordian.

19 Brightia sp. B, (type 1232B), M-7745, x 1, G. Maghara, top Zohar Fm., Up. Callovian.

20 Brightia metomphala (Bonarelli), (type 1385), M-7745:l. x 1, G. Maghara, top Zohar Fm., Up. Callovian.

21-22 Distichoceras bicostatum (Stahl), (type 1384), M-7745, x 1, G. Maghara, top Zohar Fm., Up. Callovian.

23-24 Bightia sp. cf. B. taeniolata (Bonarelli), (type 1391), M-7745:l, x 1, G. Maghara, top Zohar Fm., Up. Callovian.

25-30 Levanticeras levantinense nov. gen. and sp. (type 1205), Up. Callovian. 25. M-5362, Makhtesh Hatira, middle part of Tsia Mbr., upper Zohar Fm., x 1, ornament of inner volution. 26. M-7261, x 1, coarse ribbing of the adult stage, G. El-Minshera, upper Zohar Fm., unit 5. 27-30. M-7814, same provenance as Figure 2b, x 2, young stage with weak ventrolateral shoulders and an open umbilicus. PLATE 1

Z. LE W Y GSI Bull. 76, 1983 EXPLANATION OF PLATE 2

Levanticeras levantinense nov. gen. and sp., (type 1205), Makhtesh Hatira, middle Tsia Mbr., upper Zohar Fm., Up. Callovian. 1. M-7813, holotype, x 2/3; low, broad ribs on phragmocone. 3. M-7813, holotype, x 1; cross-section of inner volutions with an acute venter. 4. M-5385, x 1, like Figure 3.

Pachyerymnoceras philbyi (Arkell), (type 1208), x 1, HU-30980, Makhtesh Hazera, upper Zohar Fm., Up. Callovian (coll. E. Nevo); part of the specimen in PI. 3, Fig. 10.

Levanticeras sinaiense nov. gen. and sp., (type 1206), x 1, M-7261, holotype, G. El-Minshera, upper Zohar Fm., unit 5 (coll. Z. lewy); note fine, low ribbing and denticulated sutures.

Pachyerymnoceras philbyi (Arkell), (type 1208), x 1, USNM-163618, ' Aramco locality L-942, top Dhruma Fm., Jebel Tuwaiq, central Saudi Arabia (refigured from Imlay, 1970, pi. 2, fig. 12); the most complete P. philbyi showing the morphological changes between the adult and the gerontic stages. Up. Callovian. PLATE 2

LEWY GSI Bull. 76, 1983 EXPLANATION OF PLATE 3

Pachyerymnoceras levantinense nov. sp., (type 1207), M-5362, holotype, Makhtesh Hatira, middle part of Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab); x 1, complete gerontic specimen with an Erymnoceras-like phragmocone and a Pachyceras-like gerontic body-chamber.

Pachyerymnoceras levantinense nov. sp., (type 1207), M-5304, Makhtesh Hatira, lower part of Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab); x 1, several views of a young stage.

Pachyerymnoceras levantinense nov. sp., (type 1207), HU-30979, Makhtesh Hatira, lower part of Tsia Mbr., upper Zohar Fm., Up. Callovian.

Pachyerymnoceras philbyi (Arkell), (type 1208), HU-30980, Makhtesh Hazera, upper Zohar Fm., Up. Callovian, (coll. E. Nevo); see cross-section of the younger fragment in PI. 2, Fig. 2. P LA T E 3

LEWY GSI Bull. 76, 1983 EXPLANATION OF PLATE 4

Figures

1-2 c f."Erymnoceras’ coronoides (Quenstedt), (type 1204), M-5302, Makhtesh Hatira, lower part of Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab); end of phragmocone and begining of body-chamber, x 2/3.

3 Pachyerymnoceras sp. cf. P. jarryi (R. Douville), (type 1380), M-7745, G. Maghara, top Zohar Fm., Up. Callovian, (coll. M. Goldberg); same specimen as in P1.5, Fig.l; x 1.

4 Pachyceras lalandeanum (d'Orbigny), (type 1386), M-7745:l, G. Maghara, top Zohar Fm., Up. Callovian, (coll. M.Goldberg); x 2/3.

5 Pachyceras crassum R. Douvill^, (type 1387), M-7745, G.Maghara, top Zohar Fm., Up. Callovian, (coll. Z. Lewy). P LA T E 4

Z. LE W Y GSI Bull. 76, 1983 EXPLANATION OF PLATE 5

Figures

1 Pachyerymnoceras sp. cf. P. jarryi R. Douvill^, (type 1380), M-7745, G. Maghara, top Zohar Fm., Up. Callovian, (coll. M. Goldberg); x 1.

2-4 Pachyceras spathi nov. sp., (type 1249), M-7691, holoype, Makhtesh Hatira, base Be'er-Sheva Fm., Up. Callovian, (coll. M. Goldberg and M. raab); x 2/3, change in ornament and whorl-section between the adult and the gerontic stages.

5-6 Pachyceras robustum nov. sp., (type 1390), M-7745:l, G. Maghara, top Zohar Fm., Up. callovian, (coll. Z. Lewy); x 1, prorsiradiate ribs forming a V-shaped projection on the venter (compare to Pachyerymnoceas in Fig. 1). 5: holotype. PLATE 5

GSI Bull. 76, 1983 LEWY EXPLANATION OF PLATE 6

Pachyceras robustum nov. sp., (type 1390), same specimen as in PL 5, Fig. 6, holotype, x 2/3.

Pachyceras sp., (type 1367), M-5339, Makhtesh Hatira, middle Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab), x 2.

Kirikeliniceras sp. cf. K. kinkelini (Dacqu^), (type 1223), M-7671, Makhtesh Hatira, upper Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab); strong ventrolateral ribs weakening on the siphonal region.

Rursiceras sp.A, (type 1307), M-6065, Makhtesh Hatira, middle Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab); 5: right side of a fragment from Fig. 6.

"Prorsiceras hatirae nov. sp., (type 1210), Makhtesh Hatira, upper part of Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab), x 2; 7-9: M-6089, holotype, with preserved rostrum 10-11: M-5384, larger dimensions of a gerontic stage.

Pachyceras magharense nov. sp., (type 1392), M-7745, holotype, x 2/3, G. Maghara, top Zohar Fm., Up. Callovian, (coll. M. Goldberg). P LATE 6

LEWY 3SI Bull. 76, 1983 EXPLANATION OF PLATE 7

Figures

I-6 cf. Lamberticeras henrici (R. Douvill^), (type 1209), Makhtesh Hatira, Tsia mbr., uppr Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab), x 1; 1-3: M-5397; 4-6: M-5346.

7 cf. "Quenstedtoceras" sp., (type 1306), M-7261, G. El-Minshera, upper Zohar Fm., unit 5, Up. Callovian (coll. Z. Lewy), x 2.

8-10 Reineckeites sp. cf. R. douvillei Steinmann, (type 1365), M-5397, Makhtesh Hatira, lower Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. Z. Lewy), x 1; 10: corroded specimen associated with the fragment in Figs. 8-9 and attributed to the same species.

II-12 Collotia sp., (type 1377), M-7746, Maghara region (G. Hamir), top Zohar Fm., Up. Callovian, (coll. Z. Lewy); x 1; 11: cross-section; 12: ventral view.

13-14 Subgrossouvria sp. (type 1380), top Zohar Fm., Up. Callovian, (coll. Z. Lewy), x 1; 13: M-7746, G. Maghara region (G. Hamir); 14: M-7745, G. Maghara.

15 Grossouvria sp., (type 1368), M-7815, Makhtesh Hatira, lower part of Be'er-Sheva Fm., Up. Callovian, (coll. M. Goldberg and M.Raab), x 1.

16-21 Peltoceras trifidum (Quenstedt), (type 1224), Makhtesh Hatira, upper Tsia Mbr., upper Zohar Fm., Up. Callovian, (coll. M. Goldberg and M. Raab); 16-17: M-7664, x 1, note narrow, assymmetric first lateral lobe; 18 : rubber cast of M-G046, x 1; 19-21: M-5451, x 2.

22 Alligaticeras sp. cf. A. raguini (Gerard and Contant), (type 1389), M-7745, G. Maghara, top Zohar Fm., Up. Callovian, (coll. Z. Lewy). PLATE 7

LEWY GSI Bull. 76, 1983 EXPLANATION OF PLATE 8

Figures

1-2 Alligaticeras sp. cf. A. raguini (Gerard and Contant), (type 1389), top Zohar Fm., Up. Callovian, (coll. Z. Lewy); 1: M-7852, G. El-Minshera, x 8/9; 2: M-7745:l, x 1 .

3 Rursiceras sp. B, (type 1445), M-7746, G. Maghara region, (G. Hamir), top Zohar Fm., Up. Callovian, (coll. Z. Lewy); x 1.

4-6 Euaspidoceras ferrugineum Jeannet, (type 1375), M-7745, G. Maghara, top Zohar Fm., Up. Callovian (coll. Z. Lewy); and of phragmocone and begining of body-chamber, x 1.

7 "ParaspidocerasP sp., (type 1306), M-6025, Makhtesh Hatira, lower part of Be'er-Sheva Fm., attributed to the Up. Callovian, (coll. Z. Lewy); see whorl-section in Fig. 6E. PLATE 8

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