the larger benthic f oraminifera and stratigraphy of the upper jurassic/lower cretaceous of central...

REVUE DE MICROPALI~ONTOLOGIE Vol. 44, n ° 3, septembre 2001, pp. 215-232

THE LARGER BENTHIC FORAMINIFERA AND STRATIGRAPHY OF THE UPPER JURASSIC/LOWER CRETACEOUS

OF CENTRAL LEBANON

LES GRANDS FORAMINIFE, RES BENTHIQUES ET LA STRATIGRAPHIE DU JURASSIQUE SUPERIEUR

ET DU CRETACE INFERIEUR DU LIBAN CENTRAL

By Germaine NOUJAIM CLARK* and Marcelle K. B O U D A G H E R - F A D E L * *

ABSTRACT. - Calcareons agglutinating foraminifera and other larger benthic foraminifera from two formations in central Lebanon confirm the presence of Late Jurassic and Early Cretaceous age carbonates below the continental Lower Cretaceous "basal sandstone". The lowermost formation, the Bikfaya Formation, is characterized by the presence of Buccicrenata sp., Alveosepta (Redmondellina) power.si (REDMOND), A. (A ) jaccardi (SCHRODT), Pseudospirocyclina maynci HOTTINGER and Rectocyclammina chouberti HOTTINGER of I~dmmeridgian age ~ while the overlying Salima Formation is characterized by Everttcyclammina kelleri (HEINSON), E. contorta REDMOND, Bramkampella arnbica REDMOND and Riyadhella regularis REDMOND of Berriasian age. Trocholina alpina (LEUPOLD) and Nautiloculina oolithiea MOHLER and REICItEL are long-ranging species which occur throughout the Salima Formation, whereas Neotrocholina valdensis REICHEL of Berriasian

- Valanginian age appears in the upper beds of the formation below the "basal sandstone". The resulting assemblage compares closely with taxa described from lraq, the United Arab Emirates and Sandi Arabia, and confirms for the first time in central Lebanon a Kimmeridgian age for the basal 25 in of the Bikfaya Formatmn and a Berriasian-Valanginian age for the Salinm Formation.

REStnVr~. - La pr6~ence de foramimf~res calcaires agglutin6s et d'autres esp~ces de grands h~raminif~res benthiques dans deux formations carbonat6es du Liban Central conf'irme la pr6sence du Jurassique sup6rieur et du Cr6tac6 inferieur au-dessous des "Gr6s de base". La formatmn inf6rieure, ou formation de Blkfaya, est caract6ris6e par la pr6sence de Buccicrenata sp., Alveosepta (Redmondellina) powersi (REDMOND), A. (A)jaccardi (SCHRODT), Pseudospirocyclina maynct t[OTTINGER et Rectocyclammina chouberti HOTTINGER du Kimmeridgien ; au dessus, la formation de Sahma est caract6ris6e par la pr6sence d'Everticyclammina kelleri (HENSON), E, contorta REDMOND, Bramknm- pella arabica REDMOND et Riyadhella regularis REDMOND du Berriasien. D'autrcs espbces dont l'extcnsion stratigraphique est plus longue tel- les que Trocholina alpina (LEUPOLD) et Nautiloculina oolithica MOHLER et REICHEL sont pr6sentes dans route la formation de Sahma, tandls que Neotrocholina valdensis REICHEL'd'Rge Berriasien-Valanginien n'est pr6sente qne dans les niveaux sup6rieurs de la formation au-dessous des "Gr~s de base". Cette assocmtion qui est comparable h celle d6crite en lraq, aux Emirats Arabes Unies et en Arabic Saouditc, indiqnc un Rge kimmeridgien pour la pattie inf6rienre (25 m) de la formation de Bikfaya et permet de mettre en 6vidence, pour la premiere lois, la pr6- sence du Berriasien-Valanginien dans les caleaires de la formation de Salima an Liban Central.

Key-words : Largcr benthic foraminifera - Late .lurassic-Early Cretaceous - Kimmeridgian-Valanginian - Ccntral Lebanon.

Mots-cl6s : Grands foraminifbres benthiques - .I urasslque Sup6rieur-Cr6tac6 lnf6rieur - Kimmeridgicn-Valanginien - Liban Central.

INTRODUCTION

Until now Lower Cretaceous sediments of the East Mediterranean unstable outer shelf (Beydoun, 1988)

have been dated as being deposited after the uplift, erosion or non-deposition of the terminal beds of the Upper Jurassic carbonate platform. Results obtained from continuous sampling and systematic microfau- nal study of the Bikfaya Formation and the Salima

* Independent Consultant Scdimentologi,~t and Carbonate Petrologist, 186A Chartridge Lane, Chesham, Bucks, HP5 2SE, U.K. ** Postgraduate Unit of Micropaleontology, Department of Geological Sciences, University College London, Gower Street, London

WCtE 6BT, U.K.

216 LARGER FORAMINIFERA FROM LEBANON

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Affleurements jurassiques dans le Liban central, et localisation de l'atre dtudi6e.

Formation below the ?Neocomian "basal sandstone" (Dubertret , 1975, p. 363 ; Beydoun, 1977, p. 328) in central Lebanon at the locality of Bikfaya and its immediate vicinity (Fig. 1,2) challenge this view. They place the advent of Early Cretaceous sedimentation during the last phases of carbonate production, preceding uplift and erosion of the platform prior to deposition of continental fluvio-dehaic elastic sediments.

Regionally, the Jurassic unstable outer shelf (out- cropping in today 's Mount Lebanon chain) was subjected to two phases of differential uplift and erosion : 1. The first phase occurred during and after Kimmeridgian time whilst the stable inner shelf (Iraq, I ran , Gulf states, Saudi Arabia)was subjected to evaporite and dolomite sedimentation; 2. The se- cond phase occurred during and after Berriasian - Valanginian time affected the unstable outer shelf whilst the inner stable platform was exposed to normal marine carbonate sedimentation.

In the past the locally adopted lithostratigraphic nomenclature of the uppermost and terminal Juras- sic (Dubertret 1963; 1975) in Mount Lebanon had distinguished two lithological units of Kimmeridgian and Kimmeridgian/Tithonian age. They were from the base : J6 (Bikfaya Formation) comprising a 60m succession of massive to thick blue grey limestones and dolomitic limestones (Kimmeridgian), overlain by J7 (Salima Formation) with an average 30 m succession of medium ochre limestones interbedded with ochre to grey marls, and chocolate shales (Kimmerid- gian/Tithonian).

In this paper , the terminology of J6 and J7 lithological units has been abandoned, to avoid any Juras- sic connotation to the terminal carbonates under-

lying the continental "basal sandstone", and instead the names Bikfaya Formation and overlying Salima Formation (Dubertret, 1975, p. 359) are strictly ad- hered to. In the study area, the Bikfaya Formation is described from the two localities of Bikfaya and Naas (Fig. 2). The Salima Formation is described and sampled from Bikfaya locality where it is in contact with the underlying Bikfaya Formation and the overlying "basal sandstone", and at Naas its base above the underlying Bikfaya Formation was sampled and studied.

In our area of study of about 21 km 2 (Fig. 2), the Bikfaya locality has the thickest sequence of both the

Fig. 2. - Simplified geological map of area of study and location of the three measured sections of Bikfaya and Naas localities (after Dubertret, 1956).

Carte gd, ologique simpl~[6e de la r~gion 6tudi6e et emplacement des trois sections mesur6es pros de Bikfaya et Naas (d'apr~s Du- bertret, 1956).

NOUJAIM CLARK and BOUDAGHER-FADEL 217

Bikfaya Formation and the Salima Formation• In Naas, the Bikfaya and the Salima formations are sharply reduced in thickness and to the southwest of both locations this thickness reduction is maintained• The Salima Formation in part icular is reduced to scattered broken ochre limestone blocks underlying the "basal sandstone". The topmost beds of the Bik- faya Formation are either preserved or differentially karstified. Basalt flows interrupt the carbonate se- quences of the Salima Formation, and lignites cap its upper beds. Such geological display indicates a mul- tiphase structural control that affected the facies changes across time lines ranging from the Late Ju- rassic to the Early Cretaceous.

At present, the larger benthic foraminifera, the subject of study for biostratigraphical purposes here, have been described from the Bikfaya Formation at Bikfaya and Naas, from the Salima Formation at Bikfaya, and from the base of the Salima Formation at Naas. 160 samples were collected systematically from these two formations for thin sectioning and the specimens figured here are deposited in the Natural History Museum•

L I T H O L O G Y

The Bikfaya Formation and overlying Salima For- mation at the Bikfaya locality are the thickest exposures in Lebanon (180 m) (Fig. 3,5). The contact between them, uniquely developed here, is a submarine hardground that caps the massive grey limestones of the Bikfaya Formation. Elsewhere, such as at 1.5 km to the south west of Bikfaya in the locality of Naas, a karst surface separates the two formations (Fig. 4). At Naas, the Bikfaya Formation (25 m) is sharply reduced through subaerial exposure, where it underlies about 15-20 m Salima Formation. This rapid lateral thickness variation is ubiquitous along the Mount Le- banon chain and is believed to be related to two pe- riods of differential uplift and erosion of the carbonate platform at the end of Bikfaya Formation deposition and at the end of Salima Formation deposition.

The Bikfaya Formation at Bikfaya is a 60 m high towering tabular blue grey escarpment (Fig. 3). It ri- ses above the soft ochre coloured limestones and marls of the underlying Bhanness Complex Formation. Three prominent cliffs break the escarpment into three smaller lithological units made of massive blue ga-ey limestones, dolostones and dolomitic limestones.

The basal unit 1 (20 m) is made of massive to thic- kly bedded limestones and dolostones which include

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Fig. 3. - Schematic lithological succession of the Bikfaya Formation at the locality of Bikfaya.

Succession lithologique sch&natique de la formation de Bi£faya dans la rdgion de BiLfaya.

siliceous nodules and stylolitic bed partings towards its top. It is characterized by distinctive vertical joints, faint subhorizontal laminations close to the top, and a dense network of open mouldic pores in the middle of the unit. Individual bed textures are var ied; they range from mud-supported to grain- supported with selective reefal development. A thin centimetric clay horizon separates this unit from the overlying unit 2. Present day quarrying has exposed a broad ledge at the base of unit 2.


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Fig. 4. - Schematic lithological succession of the Bikfaya Formation at the locality of Naas.

Succession lithologique sch6matique de ht formation de BikJhya dans la r@ion de Naas.

The median unit 2 (21 m) which consists of dolomitic limestones, begins with a massive bioherm of corals, chaetitids, and stromatoporoids that are silica replaced. The bioherm is in turn overlain by cross-laminated grainstones of a large tidal channel which merges laterally into thick dolostones. Tightly peaked stylolitic structures occur in the topmost thick, fossiliferous beds of the unit and a narrow ledge separates the unit from the topmost unit 3.

Unit 3 (16 m) is composed of massive dolomitic limestones and limestones. At the base, it consists of hummocky mud mounds with irregular burrows fil- led with coarse crystalline dolomite. Finger and bul- bous stromatopores within the mounds are silica replaced. Thick mud-supported, layered beds overlie the mounds and enclose large fragmented or whole lamellibranchs, brachiopods, and a few stromatopores. The topmost bed of the unit is massive and is capped by a submarine hardground separating the underlying Bikfaya Formation from the above Sali- ma Formation. The submarine hardground surface displays a network of irregular burrows selectively cemented with coarse crystalline dolomite.

The larger benthic foranfinifera described from this section belong to samples collected in the interval from 15 m above the base of unit 1 to 10 m above the

base of unit 2. As the specimens studied here are from random thin sections of reefal limestones, the photographs are focused as sharply as the sectioned specimens will allow and the photographs are magni- fied to show the detailed structures we behcved to be significant.

The Bikfaya Formation at Naas is 25 m thick (Fig. 4) and also forms a prominent cliff in the land- scape. It displays vertical jointing but lacks the led- ges noted at Bikfaya. Bed partings are along horizontal stylolites rather than bedding planes. Three informal lithologic units are described. The basal unit (a) is 5-8 m thick and includes dolomitic limestones and limestones with textures that are predomi- nantly grain - supported with large colonial corals at the base.

The overlying unit (b) is a 7 m thick interval of mud- to grain-supported limestones bound by closely parallel stylolitic surfaces. This unit is distinguished by the presence of mouldic pores and leached horizontal burrows in the fossiliferous horizons. In addi- tion, there are abundant low amplitude peaked stylolites and siliceous bands and fiat siliceous lenses.

The topmost unit (c) is 5-8 m thick and consists of grain-supported limestones. Like the underlying unit (b), it contains siliceous bands and fiat siliceous lenses. Its top surface is karstified. The overlying Sali- ma Formation, rests with apparent conformity on the karst surface. Remnants of its basal ochre carbonates and marls are seen within present day cultivated terraces that grade upward into the "basal sandstone" of the Lower Cretaceous.

The lowermost 25 m of unit 1 and base of unit 2 from the Bikfaya Formation at Bikfaya and units a, b and c from the Bikfaya Formation at Naas corre- late, as a common biozone runs through these units in both localities (Fig. 3, 4).

The Sahma Formation at Bikfaya (Fig. 5) is a series of subhorizontal carbonates, marls, shales and volcanics that rest with apparent conformity above the submarine hardground at the top of the Bikfaya Formation. Its thickness of about 120 m is subdivi- ded into five distinctive lithologic units.

The lowermost unit 1 (43 m) is made of medium sized (20 cm-70 cm) ochre bioclastic and /or pelletic, oolitic grainstones interlayered with ochre-grey marls (50 cm-2.5 m) or chocolate shales. The carbonate grainstones stand out as resistant beds that separate the exposures of ochre marls and/or chocolate shales. They display low angle cross-bedding and/or subhorizontal laminations and their top surfaces are criss-crossed by a network of horizontal thalassinoid burrows. The ochre marls are fossiliferous with as-

NOUJAIM CLARK and B O U D A G H E R - F A D E L 219

~ , r~ 5 • . . . . . ~ i cover ]

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Fig. 5. - Schematic lithological succession of the Salima Formation at the locality of Bikfaya. S u c c e s s i o n l i t ho log ique s c h d m a t i q u e de I n f o r m a t i o n de S a l i m a d a n s la rdg ion de B i k f a y a .

semblages typ ica l of shallow mar ine condi t ions , with c r ino id stems, small t e r eb ra tu l i d s , gas t ropod shells and bioclas t ic debr i s . The chocolate shales a re thin hor izons devoid of macrofoss i ls .

Uni t 2 (29 m) is an in te rva l of p a r t i a l cover , wea- the red basa l t s , chocolate shales and n o d u l a r ochre limestones b locks of gra ins tone tex ture .

Uni t 3 of 20 m is a massive cliff in field view. I t is i n t e r p r e t e d as a c a rbona t e (coarse oolitic and bioclastic) sand ba r . Its uppe rmos t hor izon is lignitic and contains the f i rs t inf lux of si l t-sized subangu la r qua r t z grains. This hor izon is i r r egu la r due to pa r - t ia l erosion.

Uni t 4 (about 25 m) is of d i scont inuous n o d u l a r ochre gra ins tone hor izons and grey green clay hor i - zons. Lenses of hemat i t ic r ed clays occur indica t ing the sites of deeply wea the red basahs .

The last and topmost uni t 5 (20 m) is ano the r cliff fo rming ca rbona t e sand b a r s imi lar in fabr ic to uni t 3. Sand-s ized qua r t z gra ins in the u p p e r cliff p ro - gressively increase up to 45 % of const i tuents before they decrease in the u p p e r m o s t s t r a t a immedia te ly below the "basa l sands tone" . The fluvio - del taic "basa l sands tone" (Tixier , 1971, 1972) d rapes the topmost bed of uni t 5. La te ra l ly , 500 m to the nor- theas t of the s tud ied sect ion in a d ry wadi bed , the contac t of Sal ima ca rbona tes and the "basa l sand-


stone" appears as a tidal channel infilled with limestones that grade upward into quartz sandstone.

Benthic foraminifera are described f rom : (a) the carbonate grainstone beds of unit 1, and (b) the massive coarse grainstone beds of units (3 and 5).

Benthic foraminifera f rom the basal horizon at Naas are described to compare and contrast with those of the Salima Formation at Bikfaya to the north and those recorded from the Salima Formation at Broumana to the south (see Fig. 2).

S Y S T E M A T I C D E S C R I P T I O N

Suborder TEXTULARIINA DELAGE and H E R O U A R D , 1896

Superfamily L I T U O L A C E A d e B L A I N V I L L E 1827 Family H A U R A N I I D A E S E P T F O N T A I N E , 1988

Subfamily A M I J E L L I N A E S E P T F O N T A I N E , 1988

Remarks : The taxonomic revision proposed by Septfontaine (1988) for the lituolids is followed in this paper.

Genus Alveosepta H O T T I N G E R , 1967 Subgenus Alveosepta H O T T I N G E R , 1967

Alveosepta (Alveosepta) j accard i (SCHRODT, 1894) (Pl. 1, fig. 3, 6, 9)

1894. - Cyclammina jaccardi SCHRODT. -- p. 734, tfs.

1928. -- Pseudocyclammina personata TOBLER. -- p. 213, pl. 24, fig. 1-3.

1938. -- Pseudocyclammina sequana (Merian) var . minor MOrILER. - p. 16, pl. 1, fig. 5-6.

1938. - Pseudocyclammina sequana (Merian) var . major MOHLER. -- p. 16, pl. 1, fig. 3-4.

1 9 6 4 . - Pseudocyclammina jaccardi ( S C H H O D T ) . - - Redmond , p. 406, pl. 1, fig. 2 -4 : pl . 2, fig. 3-4.

1967. - A l v e o s e p t a jaccardi ( S C I t R O D T ) . - - Hot t inger , p. 79, pl. 15, fig. 15-16.

1967. - Alveosepta jaccardi personata (MOHLER). -- Hot t inger , p. 80, pL 15, fig. 1-3.

1981. - Alveosepta jaccardi (SCHRODT). - Sept fonta ine , p. 198, fig. 5, 6.

1984. - Alveosepta jaccardi (ScI-IRODT). -- P61issi~, et al., p. 486, pl . 22, fig. 4.

1988. - Alveosepta jaccardi ( S C H R O D T ) . - Sept fon tame , p. 244.

1991. - Alveosepta (Alveosepta) jaccardi ( S C H R O D T ) . - - B a n n e r and W h i t t a k e r , p. 42.

Material and dimensions : 10 specimens, greatest diameter. 1.80 mm in megalospheric generations.

Remarks : A. (A.) jaccardi has the alveoseptid "clear line" of resorption (see Septfontaine, 1981, p. 198, fig. 6) and the areal cribrate aperture. Unlike A. (R.) powersi, it lacks tile pillar structures of the septa that project into the chambers.

The specimens of A. (A.) jaccardi ( S C H R O D T ) , P .

sequana TOBLER, P. sequana major MOHLER and P. sequana minor MOHLER seem to be indistinguishable in practice. Attempts have been made (e.g. Mohler, 1938, op. cit. ; Hottinger, op. cit., 1967) to distinguish some or all of them quantitatively (e.g. chamber height/ length, rate of spire diameter increase) and statistically. The quantitative distinction is shown by the microspheric forms (see Hottinger, 1967, op. cit.), but is not clear in the megalospheric forms as the progressions seen in one locality may he inverted in another.

Distribution: This species was first described from the Late Oxfordian of Switzerland (Maync, 1958), and was also reported from the Late Oxfor- dian of Israel (Maync, 1965). Elsewhere in the

P L A T E 1

1, 4. Rectocyclantmina chouberti HOTTINGER~ [{ammeridgian, ayaal sect ions, 1 : Sample 2N, x 83 ; 4. Sample 2N, x 40. Top bed of B ik faya F o r m a t i o n below k a r s t m Naas.

3, 6. Alveosepta (Alveosepta) jaccardi (ScHRODT), Kimmer ld- g i a n . - Ahnost equa to r i a l sections of megalospher ic genera t ions. 3 : Sample 6 (3), x 25 ; 6. Sample 4N, × 40. Top of 25 m above base of B ik faya F o r m a t i o n at B ik faya and top 20 m above base of B ik faya F o r m a t i o n at Naas.

9. Alveosepta sp. An equa to r i a l sect ion of a morpholog ica l ly in te r - med ia te fo rm between Alveosepta s.s. and Alveosepta (Red- mondellina), Sample 6(3) B, x 79. Same level as above at B ik faya and Naas.

2, 8, 11. Alveosepttl (Redmondellina) powersi (REDMOND, 1964), ax ia l sect ions, al l showing the a lveosept id "c l ea r l ine" and the "med ian l amel la" 2 : Sample aB, x 25 ; 8 : Sample 4N, x 39 ; 11 : Sample 4N0 × 64. Kimmerdg ian . Same level as above at B ik faya and Naas.

5, 7, 10, 12. Pseudospirocyclina maynci HOTTINGER, 1967, Kiln- mer idg ian , ax ia l sect ions of mega lospher ie genera t ions , al l showing the s t rong, s epa ra t ed p i l l a r s c lus te red in med ian zone. 5 : Sample 4N, × 64 ; 7 : Sample 4N, x 64 ; 10 : Sample a(3) B, x 43 ; 12 : Sample 4N, x 43. Same level as abovc at B ik faya and at Naas.

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222 LARGER F O R A M I N I F E R A FROM LEBANON

Middle East, it was noted f rom the Early Kimmerid- gian of the Jubai la Format ion (Hottinger, 1967; Banner and Whit taker , 1991) and the Hanifa Forma- tion of Saudi Arabia (Redmond, 1964). In the northern extension of Mount Lebanon at Jibal AI Sahiliyah, it was recorded from the Upper Oxfor- d ian/Kimmeridgian (Fourcade and Mouty 95) of Wadi A 1 0 u y o u n . Elsewhere in the Tethys, it was ci- ted f rom the Kimmeridgian of the Pyrenees of France, and f rom the Late Oxfordian to the Ear ly Kimmeridgian of Morocco (Hottinger, 1967). A. personata was first described f rom the Kimmeridgian of Switzerland (Tobler, op. cit.), while P. sequana major and P. sequana minor were both described f rom the Late Oxfordian of Switzerland. The species was recorded f rom the lower beds of the "Couches Jaunes Infer ieures" equivalent of the Bhanness Formation (Bischoff, 1964). Its age range in Mount Lebanon extends f rom the Upper Oxfordian - to Mid Kimmerid- gian. In central Lebanon, it is described here front the Bikfaya Format ion at Bikfaya (24 m from base), and at Naas (17 m from base).

Kimmeridgian of eastern Morocco. The figured specimens are f rom the basal 25 m of the limestones of the Bikfaya Format ion at Bikfaya and f rom the basal 23 m of the same formation at Naas (for their faunal associations and position see fig. 3,4). This species was first described f rom the Kimmeridgian of the Upper Jnbai la Format ion. Hot t inger ' s specimens came f rom the Upper Jurassic, Kimmeridgian of eastern Morocco in association with Karnubia and Cly- peina jurassica.

Simmons and A1 Thour (1994) recorded this species f rom the mid Early Kimmeridgian of Yemen. Clark and BouDagher-Fadel (in press) figured specimens fl 'om the Kimmeridgian of the Bikfaya Forma- tion in Central Lebanon (Naas locality). Similarly to A. (Alveosepta) jaccardi it has presently been described f rom the Upper Oxfordian / Basal Kimmeridgian to the uppermost Ear ly Kimmeridgian of the Bhan- heSS Formation. Thus its age range inclusive of its appearance within the Bikfaya Format ion in Mount Lebanon extemls f rom the Upper Oxfordian to the Mid Kimmerdgian.

Subgenus Redmonde l lh la BANNER and WIIITTAKER, 1991

Gcnus Pseudosp i rocyc l ina IIOTTINGER, 1967

Alveosepta (Redmondel l iua) powersi (REDMOND, 1964)

(PI. 1, fig. 2, 8, 11)

1964. - P~eudocyclcnnmina pott~er.~i REDMOND. - - p. 406-4007, pl. 1. fig. 5-8 ~ 171. 2. fig. 5-8.

1967. - Alveo~epta powersi (REDMOND). -- Holtmger° p. 81-83, text-fig. 41-42 ; pl. 1, fig. 15 ; pl. 16, fig. 20 ; pl. 17, fig. 1-16 " pl. 18, fig. 1-12.

1991. - Alveo~epta (Redmo,dellina) powersi (REDMOND). - Ban- ner a~/d Whittaker, p. 43, pl. I, fig. 1~8.

Material and dimensions : 72 specimens, greatest diameter 1.85 mm in microspheric generations.

Remarks : This species is distinguished by a cont- pressed test with pillar-like hypodermal extensions linking the septal hypodermis to the anter ior of the epidermis of each preceding septum. Division of the hypodermal alveoles produces finer and finer alveoles distally, as they bifurcate or tr ifurcate (twice) ap- proaching the epidermis (P1. 1, fig. 8). The pillars are present only in the median, equatorial plane (Pl. 1, fig. 2), not spread throughout the chamber space as in Pseudospirocyclina maynci I]OTT[NGER (PI. 1, fig. 5,7).

Distribution: This species was first described f rom the Kimmeridgian of the Upper Jubai la Forma- tion of Arabia. Hot t inger 's specimens came f rom the

Pseudosp i rocyc l ina mayuc i HOTTINGER, 1967 (PI. l , fig. 5, 7, 10, 12)

1967.- Psettdospirocycli,a maynci [IOTTINGER. - p. 70,72, pl. 12, fig. 1-17 : p. 71, text-fig. 36.

Material and dimensions : 60 specimens. 2.5 mnt greatest diameter.

Description : P. maynci differs f rom Alveosepta (Redmondellina) po'wersi by : the coarser hypoder- real s t ructure ; flaring (peneropliform) test or rectili- near development ; much stronger separated pillars through the whole chamber lumen (not merely in the median plane) and the absence of septal "clear-line".

Septfontainc (1988, p. 244) stated that Pseudospi- rocyclina is "probably a synonym of Anchispirocycli- na JORDAN and APPLIN, 1952", however, Pseadospi- rocyclin<t has a more simple internal s t ructure and a planispiral test throughout and is not considered a synonym here.

Distribution : P. muynci was first described f rom the Upper Jurassic, Kimmeridgian of eastern Moroc- co. The figured specimens appear in conjunct ion wi th the Alveosepta (Redmondel l ina) powersi (REDMOND) at the same levels of the Bikfaya Forma- tion at Bikfaya and Naas.


Family CYCLAMMINIDAE MARIE, 1941 Subfamily BUCCICRENATtNAE LOEBLICH

and TAPPAN, 1985

Remarks : The genus Buccicrenata is placed in the Cyclamminidae following the systematic revision of Loeblich and Tappan (1985 ; 1988) and the taxonomic and strat igraphic emendation of BouDagher- Fadel (in press). Loeblich and Tappan (op. cit.) de- nied the presence of alveolae in the septum of Bucci- crenata. However , BouDagher-Fadel (op. cit.) in examining numerous randomly thin-sectioned specimens of Buccicrenata f rom different localities, some of them hypotypes deposited in the Natura l History Museum, demonst ra ted that alveolae existed both in wall and in the septmn. These characters were used previously by Banner and Highton (1990) to distinguish Buccicrenata f rom Everticyclammina. Bou- Dagher-Fadel (in press) has also emended the full s trat igraphic range of Buccicrenata to include the I( immeridgian to Cenomanian, placing its origin in the Upper Jurassic of the Middle East.

Genus B u c c i c r e n a t a LOEBLICH and TAPPAN, 1949

Bucc icrenata sp. (P1. 3, fig. 4)

Material and dimensions : 5 specimens, greatest length observed 2.3 mm.

Remarks : The genus Buccicrenata LOEBLICH and TAPPAN (1949, emended 1985, p. 100) extends geo- graphically f rom Nor th America to the Middle East. Buccicrenata sp. is a primitive form of Buccicrenata hedbergi (MAYNC, 1953) and could be the ancestral form of this early Cretaceous species. It seems to grade gradually f rom its ancestor Everticyclantmina, which has an alveolar hypodermis and a single, areal , " ammobacu l i t i d " scptal / terminal ape r tu re , into a more advanced form with alveolar septa which extend from the lateral chamber walls. Buccicrenata sp. has the long, low reniform chambers in the planispiral por t ion with four to five chambers per whorl as seen in B. hedbergi. The hypodermis is distinctive- ly thick with coarse alveoli which bifurcate i rregular- ly. However , as in Everticyclammina, the septa are still solid in the early whorls, acquir ing the alveoles gradual ly towards the last par t of the test. The septa of the last two chambers of the planispire stage are typical of those of Buccicrenata, thus making this species a morphological link hetween Everticyclam ,dna and Buccicrenata. The few long and low chambers, the weakly alveolar septa and the thick hypodermis distinguish this species f rom lcalown species of both Everticyclammina and Pseudocyclammina.

Distribution : As this fo rm is of Kimmeridgian age, it is the oldest known immediate ancestor of the Valanginian - Albian Buccicrenata hedbergi. To eva- luate this species fully more specimens are needed and the genus will be fully reviewed in a separate paper. The specimens described here are f rom a sample collected at 6 m above the base of the Bikfaya For- mation at Naas.

Family EVERTICYCLAMMINIDAE SEPTFONTAINE, 1988

Genus Eve r t i cyc l ammina REDMOND, 1964

Eve r t i cyc l ammina kelleri (HENSON, 1948) (P1. 2, fig. 1-4; PI. 3, fig. 1,3)

1948. - Pseudocychtmmina kelleri HENSON. -- p. 16-17; pl. 9, fig. 4,5,7.

1964. -- Everticyclammina eccentrica REDMOND. -- p . 4 0 8 , pL l, fig. 16-18; pl. 2, fig. 12-13.

1964. - Everticyclammina elegans REDMOND. - - p . 408-409, pl. 1. fig. 19-20; pl. 2, fig. 14-16.

1990. - Everticyclammina kelleri (I~ENSON). -- Banner and High- ton, p. 6. pl. 1, fig. 2-6 ; pl. 2, fig. 1-4 ; pl. 3, fig. 1-2.

1991. - Everticyclammina kelleri ( H E N S O N ) . -- Banner and Whit- taker, p. 50, pl. 4, fig. 4-11 ; pl. 5, fig. 1-4.

Material attd dimensions : 65 specimens, greatest length observed 3.5 mm.

Remarks : E. kelleri was redescribed and a lecto- type defined by Banner and Highton (1990) who considered both E. eccentrica and E. elegans to be its synonyms. E. kelleri has a smooth, regularly s t ructured hypodermis with much finer alveolae than its ancestral E. praekelleri BANNER and HIGHTON (1990, p. 8, pl. 1, fig. 1 ; pl. 3, fig. 5 ; pl. 4, fig. 1-11). E. praekelleri is recognisable by its enlarged hypodermal alveolae with a tendency to few chambers per whorl , and is of IGmmeridgian-Ti thonian age. The latter was formally described by Banner and Highton (1990, p. 8) f rom central Lebanon (4 km south west of Bikfaya village on the road between Bhannes and Dahr E1 Souan) where it was collected f rom limestone blocks in the ochre marls of the Salima Formation. Our material of E. kelleri is f rom the lower beds of the Salima Format ion at Bikfaya.

Distribution : E. kelleri was originally described f rom the subsurface of Awasil well No.5, I raq , fi 'om the stratotype Zangura Format ion (Dunnington et al., 1959, p. 305-306), of Bcrr iasian-Valanginian age (Banner and Highton, 1990). The specimens described here came f rom the units 1 and 5 of the Salima Format ion at Bikfaya.

224, LARGER FORAMINIFERA FROM LEBANON

Ever t ieyclammina eontor ta [{EDMOND, 1964 (PI. 2, fig. 5-6)

1964. Everttcychtmn~ina contorta REDMOND. - p. 408, pl. 1, fig. 12-15 ; pl. 2, fig. 10 11.

1 9 9 1 . - Everticyclammina contorta REDMOND. -- Banner and Whiitakcr, p. 48, pl. 3, fig. 5-7; pl. 4, fig. 1-3.

Material and dimensions : 38 specimens, maximum length observed 3.8 mm.

Remarks : This species was differentiated from Everticyclammina greigi HENSON (1948) by Red- mond (19641 and by Banner and Whittaker (1991) by its possession of few chambers per whorl, by its septa that meet the per iphery obliquely in equatorial section (P1. 2, fig. 5) and by its inner whorl surface, which increasingly meets the inner whorl at right angles (Banner and Whittaker, 1991, p. 48, pl. 4, fig. 3 ; this paper P1. 2, fig. 6). The species is close to the ancestral E. virguliana (KOECHLIN, 1942) but the latter has more chambers per whorl and simpler, non-bifurcat ing hypodernta l alveoles (Hott inger , 1967 ; Banner and Highton, 1990 ; Banner and Whit- taker, 1991)

Distribution : The type species of E. contorta was obtained by Redmond (1964) from the Buwaib For- mation of Saudi Arabia. It is characteristic of the Berriasian-Valanginian to the Lower Barremian of Arabia (Banner attd Whittaker, 1991). The present specimens are from the lower lithologic unit 1 of the Salima Formation at Bikfaya.

Genus Rec tocye lammiua H O T T I N G E R , 1967

Rectocyclalnmina chouber t i H O T T I N G E R , 1967 (P1. 1, fig. 1,4)

1967. - Rectocyclamrntna ehouberti [|OTTINGER. pl. 9, fig. 19 21 ; text-fig. 26a-b, 27 a c.

Material and dimensions : 28 specimens. Greatest diameter 1.5 mm.

Remarks : R. chouberti is distinguished by a long cylindrical test with a planispiral early stage and very narrow hypodcrmal alveoles. This species is placed here in the Everticyelamminidae following the classification of Septfontaine (1988, p. 249).

Distribution : The type specimens of R. chouberti came from the Upper Jurassic, Kimmeridgian of Eas- tern Morocco. The present specimens have been described from 23 m front the base of the upper beds of the Bikfaya Formation at Naas and immediately below the karstified topmost beds, unit c. (Fig. 4).

Subfamily CHOFFATELLINAE MAYNC, 1958

Genus Bramkampel la REDMOND, 1964

Bramkampel la arabica HEDMOND, 1964 (P1. 2, fig. 13-14; P1. 3, fig. 2, 5, 6, 8)

1959. - ? Haurania sp. DUNNINGTON (tn Dunnington et al.). - p. 306.

1964. - Bramkampella arabica REDMOND. p. 409-414, pl. 1, fig. 26-29 ; pl. 2, fig. 19-20, p. 409 ; text -- figure 2.

1988. -- Braml~ampella arabica REDMOND. -- Loeblich and Tap- pan, p. 101-102, pl. 100, fig. 14-18 (reproduced from Red mond, 1964).

1991. - Bramkampella arabica REDMOND. -- Banner and Whitta- ker, p. 45, pl. 2, fig. 1-7.

Material and dimensions : 75 specimens, maximum observed diameter is 1.30 mm.

Remarks : This monospecific genus is characterized by the alveolar structure of the hypodermis and by the radial partitions in the uniserial par t of the test which extend the height of each chamber from the base to its terminal aperture. Most of the alveoles divide at least once. The radial chamber partitions are inward extensions of pr imary hypodermal inte- ralveolar structures. A juvenile specimen shows the internal partitions in the last and penultimate illus- trated chambers (P1. 3, fig. 8).

Distribution: This species was first described from the upper par t of the Sulaiy Formation (Late Berriasian, possibly to Early Valanginian) of I raq and the equivalents of that formation in Saudi Ara- bia. B. arabica is not known in Upper Jurassic sedi- mcnts. Banner and Whit taker (1991, p. 45) stated that this species appears to be an index for the earliest Cretaceous, Late Berriasian to Early Valangi- nian. It lived in sheltered marine sediments. The present specimens have been described from unit 1 of the Salima Formation at Bikfaya.

S u p e r f a m i l y TEXTULARIACEA E H R E N B E R G , 1 8 3 8

F a m i l y CHRYSALIDINIDAE NEAGU, 1 9 6 8

S u b f a m i l y I~ARAVALVULININAE BANNER, SIMMONS

a n d W H I T T A K E R , 1991

Genus Riyadhella REDMOND, 1965

Riyadhella regularis REDMOND, ] 965 (P1. 2, fig. 7)

1 9 6 5 . - Riyadhella regalaris IIEDMDND. -- p. 138-140, pl. 1, fig. 32-34.

1991. -- Ri~adhella reg~ularis REDJ~tOND. -- Banner~ Simmons and Whittaker° p, 131, fig. 57-63 (scc list of synonyms).

NOUJAIM CLARK and BOUDAGIIER-FADEL 225

Material and dimensions : 54 specimens, maximum length 0.5 mm.

Remarks : R. regularis is distinguished by its high chambers (as high as broad) and smoothly curved septa. The early stage of growth is quadriserial but becomes triserial in the adult. Banner et al. (1991) revised the genus Riyadhella and its four assigned species from thin sections of type material. Their amended descriptions of the Redmond (1965) species placed R. hemeri, R. intermedia and R. nana in sy- nonymy with R. regularis. Riyadhella species are known from the United Arab Emirates and Saudi Arabia, they occur in the Kimmeridgian, trot are not present in overlying "Tithonian-Valanginian" strata that are essentially composed of evaporites and dolostones. Their occurrence in central Lebanon in the upper beds of the Salima Formation, below the "'basal sandstone", strongly suggests an age range that extends into the earliest Cretaceous.

Distribution : The type specimens of R. regularis came from the Bajocian - Bathonian of Aramco well T 60A, basal member of the Upper Dhruma Forma- tion, Saudi Arabia. The present specimens are described from the units of the Salima Formation at Bikfaya.

Riyadhella sp. (P1. 2, fig. 8)

Material and dimensions: A single specimen, maximum length 0.4 mm.

Remarks : This (so far" unique) specimen is recognisable by its very low chambers and thick septa. These features exclude it from any known species of Riyadhella, but it is left in open nomenclature until the species diagnostic characters can be confirmed from other specimens.

Distribution : This specimen has been described from the topmost unit 5 of the Salima Formation at Bikfaya.

S u b o r d e r MIL1OLINA DELAGE and HI~ROUARD, 1896 Superfamily MILIOLACEA EHRENBERG, 1839

Family NAUTILOCULINIDAE LOEBLICH and TAPPAN, 1985

Remarks : Nautiloculina had been variously placed systematically. It was originally described by Mo- hler (1938, p. 18) as calcareous and imperforate, and

compared to porcelaneous Planispirina. Locblich and Tappan (1964b, p. 443) placed the genus into the miliolids. They subsequently (1985, p. 92, 1988, p. 71) reallocated this genus into the lituolids. We do not agree with this classification as Nautiloculina does not possess a microgranular agglutinated wall. Yet, it is not a member of the calcareous rotaliines with the hyaline calcitic perforate wall. The multi- layered imperforate wall of Naatiloculiua is very difficult to separate from simple fusulinids such as the Carboniferous Millerella THOMPSON, 1942. Nonethe- less, the considerable time gap between the Palaeo- zoic Loeblichiidae and the Jurassic-Cretaceous Nautiloculinidae makes it difficult to explain the re- lationship between them. We place it here in the Mi- liolacea because some of the miliolids (such as Austrotrillina, Quinqueloculina, etc.) display double layered walls like Nautiloculina, although the thin dark layer is internal to the thick transparent layer of the wall of the normal miliolids but it is extrenal to the wall of Nautiloculina. Consequently, the thin dark layer may be basal to the wall of the normal miliolids while the later part of the wall grow inwards toward the chamber lumen; in Nautiloculiua the thin dark layer of the wall could equally be basal to the development of the thicker translucent part of the wall which also wouhl have grown inwards towards the chamber lumen.

Nautiloeulina oolitlfica MOHLER, 1938 (PI. 2, fig. I0)

1938. - Nautiloculina oohthtctt MOIILER. - p. 19, pl. 4, tig. 1-3 : p. 19, th. 6, pl. 4. fig. 1-3.

1988. - Nautiloculiua oolithica MOI-11,ER. - Loeblich and Tappan, p. 71, pl. 54, fig. 10-112 (reproduced from Mohler~ 1938).

Material and dimensions : 29 specimens, maximum measured height 0.9 ram.

Remarks : N. oolithiea is distinguished by a pla- nispirally enrolled and involute test, and a globular proloculus with heavily thickened umbilicus.

Distribution : The types were from the Oxfordian of Switzerland. N. oolithica ranges from the Middle Jurassic (Bathonian) (Dunnington et al., 1959, p. 193) up into the Early Cretaceous (Early Aptian) (Loeblich and Tappan, 1988). The present specimens came from the upper beds of the Salima Formation at Bikfaya.


S u b o r d e r INVOLUTININA H O H E N E G G E R

and PILLER, 1977 Superfamily INVOLUTINACEA Z A N I N E T T I , 1975

Family INVOLUTIN[DAE R I ) T S C H L I , 1 8 8 0

S u b f a m i l y INVOLUTININAE B U T S C H L I , 1 8 8 0

Distribution : The type specimen of N. valdensis came from the Valanginian of Arzier, western Swit- zerland. The present specimens' provenance is from the upper massive beds of unit 5 of the Salima For- mation at Bikfaya.

Genus Neotrocho l ina REICHEL, 1956

Remarks : Locblich and Tappan (1988, p. 300) considered Neotrocholina REICHEL as a synonym of Trocholina P~ALZOW. However, the two forms arc different and shouhl be separated. The outer wall of Neotrocholina is thick (approximately as thick as the spiral septum), perforate and the umbilicus is deeply fissured. On the other hand, the outer wall of Tro- cholina (= Coscinoconus alpinus LEUPOLD) is thin (usually much thinner than the spiral septum, and often eroded), imperforate, and the test lacks the deeply fissured, canaliculated umbilical structure of Neotrocholina.

Neotrochol iua valdensis REICHEL, ]956 (P1. 2, fig. 12, 15)

1956. - Neotrocholina valdensis REICHEL - p. 404, pl. 16, fig. 1, 3-5, 7 ; p. 405, tf. 5, pl. 16, fig. I .

Material and dimensions : 24 specimens, maximum measured height 0.8 ram.

Remarks : N. valdensis is characterized by a strong canaliculation on the dorsal whorl and a ven- tral umbilicus infilled with a complicated plug. It differs from N. friburgensis GUILLAUME and REICHEL, 1957 by its low coiling mode.

Genus Trochol ina PAALZOW, 1922

Remarks : Trocholina is distinguished from Neo- trocholina in having a thinner, imperforate wall, and in lacking the deeply fissured, canaliculated umbilical structure of the latter.

Trochol ina alpina ( L E U P O L D , in LEUPOLD and BIGLER, 1936)

(P1. 2, fig. 9, 11; P1. 3, fig. 7)

1936. - Coseinoeouns alpittus LEUPOLD in LEUPOLD and BIGLER. -- p. 606, pl. 18, fig. 1-11.

1948. - Trocholina intermediu HENSON. -- p. 54, pl. 11, hg. 2a- 2b ; pl. 3, fig. 10 (not T. intermedia FRENTZEN, 194[, p. 305, pl. 1, fig. 10).

1949. -- Trocholina urubtca nora.troy. HENSON. -- p. 173.

1994. -- Trocholina alpina (LEUPOLD). -- Chlocchini et al., pl. 30, fig. 1-2.

1999. - Trocholina alptuu (LEUPOLD). -- Mancinelli and Coccia, p. 150, pl. 3, fig. 1-3, 7, 8.

Material and dintensions : 68 speeimens, maximum observed height 1.8 nun.

Remarks : T. alpina is distinguished by its piano- convex test which in section shows a spiral tube characterized by its height and a spiral septum which is nearly at right angles to the solidly infilled umbilicus, but broadly oblique to the outer wall.

P L A T E 2

1-4.. Everticyclammina kelleri (IIENSON, 1948). Bcrr las iam 1 : Sample Sa. 6 ; 2 : Sample Sa. 1 ' : 3 : Sample Sa. I ' ; 4 : Sample Sa. 1", × 70. Axial sections of inegalospheric genera tions showing fine hypodermal alveolae, f rom lower and upper lithunits of Salima Format ion a! Bikfaya.

5, 6. Everticyclammina enutorta REDMOND, 196,t. Berriasian. - 5 : Sample Sa. 12(1), x 52, equatorial section of a megalospheric f o r m ; 6 : A near axial section of an megalospheric form. Saniple Sa.12(l) , x 76. F rom lower li thunit of Sahma Format ion at Bikfaya.

7. Riyadhella regularis REDMOND, 1965. Sample Sa.5(l) × 122. An axial section tk'om lower l i thnnit of Salima Format ion at Bik- faya.

8. Riyadhelht, sp. Sample Sa.g. x 110. A near axial section f rom F r o m the upper li thunit of Salima Format ion at Bikfaya.

9, 11. Trocholina alpina (LEUPOLD, in LEUPOLD and BIGLER, 1936), 9 : Axial section, Sample Sa.b. x 57 ; 11 : Near axml

section, Samt)le Sa. 1", × 50, F rom the u p p e r li thunil of Sali- ma Format ion at Bikfaya.

10. Nautiloculina oolithica MOIILER, 1938. An oblique axial sec~ tion, umbonally thickened, with "choniata" at aper tura l mar- ~ n , Samplc Sa.l". × 50. F rom the upper l i thumt of Sahln, Format ion at Bikfaya.

12, 15. Neotrocholina valdensis REICHEL, 1956. Bem'iasian-Va- langinian, 12 : Sample Sa.5' × 74; 15 : Sample Sa.f x 74. Axial sections from the upper li thnnit of Salima Format ion at Biklaya, showing the deeply fissured, canalicnlated umbilical s t ructure .

13, 14. Bramkampella arabica REDMOND, 1964, Berr iasian, 13 : Sample Sa. 12( l)~ cquatorial section of a mcgalospheric form, x 31 ; 14 : Sample Sa.12(I) , near equatorial section of a m~- crospheric form, × 35. From lower lithnnlt of the Salima For- mation at Bikfaya.

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228 L A R G E R F O R A M I N I F E R A F R O M LEBANON

Distribution : The species was f irst desc r ibed by Leupo ld (in Leupo ld and Bigler, 1936) from the U p p e r T i thon ian of the Axa lp region, Swi tzer land. Henson (1948, 1949) desc r ibed it f rom Q a t a r , Saudi A r a b i a (Dukhan) and l r a n , where it occu r red in Lo- wer Cenoman ian sediments (youngest r e c o r d e d age of this genus). Mancinel l i and Coccia (1999) r eco rded its presence in the U p p e r T i thon ian , its conmmn occu r rence in the Be r r i a s i an , and its decline in the Va- l ang in i an of the c e n t r a l / s o u t h e r n Appen ine s . T. alpina ranges down into the U p p e r Jurass ic (G19) of the Middle Eas t (Chocchini et al., 1994). The p resen t specimens a p p e a r t h roughou t the Salima F o r m a t i o n at Bikfaya .

BIOSTRATIGRAPHY

In cen t ra l Lebanon , the Late Jurass ic - E a r l y Cre taceous ca rbona te s fal l wi thin the r ea lm of the uns tab le outer shelf (def ini t ion in Beydoun , 1988, p. 2) close to the marg in of the southern Tethys. This U p p e r Jurass ic - Lower Cre taceous p l a t fo rm links to the no r theas t with the s table inne r sheff p l a t fo rm (Beydoun 1988) tha t extends f rom l r a q to the regio- na l s t re tch of the A r a b i a n Pen insu la su r round ing the posi t ive a rea of the A r a b i a n shield ( J ,De rcou r t et. at., 1985, pl. 3). A pa leohigh immedia te ly to the east of the p resen t ly s tud ied po r t i on of the ou te r uns tab le shelf (see Dercou r t et. al., pl. 3) separa tes bo th shelves, yet does not p reven t the cont inuous d i s t r ibu t ion of ben th ic fo ramin i f e ra th rough the no r theas t pas- sage way. Indeed our p resen t work shows a commo- nal i ty of l a rge r ben th ic fo ramin i fe ra species across bo th shelves. Of these f i ) ramini fera , the ca lcareous agglut inat ing Tex tu la r i ina prove the most useful as they have unt i l r ecen t ly been the subjec t of numerous works re la t ing to the i r b ios t r a t ig raph ic signifi- cance (Henson, 1948, 1949; Redmond , 1964, 1965; Sept fonta ine , 1988; B a n n e r aml Highton , 1990;

B a n n e r and W h i t t a k e r , 1991; B a n n e r et al., 1991; Maync , 1996, Bassoul le t , 1998, etc.) .

The Bikfaya F o r m a t i o n at B ik faya (units 1, and base 2) and Naas (units a, b and c) is cha rac t e r i zed in its lower 25 in uni t by a b iozone of Kimmer idg ian age conta in ing Alveosepta (Redmondellina) powersi (REDMOND), Alveosepta (Alveost, p t a ) j a c c a r d i (SCHRODT), Pseudospirocyclina maynci HOTTINGER, and Rectocyclammina chouberti HOTTINGER. The top of this biozone at B ikfaya occurs below 35 m of mass ive hmestones (Fig. 3), whereas at Naas (Fig. 4) it occurs below a k a r s t surface. Di f fe ren t ia l upl i f t and p a r t i a l exposure affects the p l a t fo rm at Naas lo- cah ty dur ing and /o r af ter K immer idg ian t ime whereas cont inuous submers ion of the p l a t f o r m at Bik- faya local i ty subjects it to c a r b o n a t e sed imenta t ion dur ing and af ter the Ifffmmeridgian unt i l p e r h a p s Ti- thonian t ime. Tol land (1997, pe r sona l communica- t ion) has po in ted to the evidence of T i thon ian deposi- t ion at B ikfaya local i ty in his s tudy of dinocysts of the Bikfaya Forn ta t ion . However , the l a rge r benth ic fo ramin i f e r a l assemblage desc r ibed he re f rom the top of the Bikfaya F o r m a t i o n and the base of the Salinm F o r m a t i o n do not conclusively cha rac t e r i ze the Ti- thon ian .

F iehl descr ip t ion shows the lower ca rbona tes of the Sal ima F o r m a t i o n at Bikfaya res t ing with appa - rent conformi ty above the submar ine h a r d g r o u n d capp ing the Bikfaya Fo rma t ion . These ca rbona te s h a d been depos i ted af te r a pe r iod of non-depos i t ion at Bikfaya . The i r l a te ra l extension to the south at Naas and B r o u m a n a i n c u r r e d deposi t ion above an e levated and e roded Bikfaya F o r m a t i o n . The resul- t ing h ia tus (depos i t ional and /o r eros ional ) between bo th format ions in the three a fo remen t ioned localities explains the T i thon ian ambigui ly in the Jurass ic s t r a t i g r a p h y of Lebanon .

Regional ly in I r a q , I r a n , Saudi A r a b i a and Oman the T i thon ian is poor ly known (Banner and Whi t t a - ke r , 1991), for it is bel ieved to be r e p r e s e n t e d by fos- s i l -poor dolostones and evapor i tes tha t ended Ju ra s -

P L A T E 3

1, 3. Everticyclammiua kelleri (HENSON, 1948). Berriasian. - 1 : Oblique axial section Samplc Sa.5(l), × 121; 3 : Oblique equatorial section of a megalospheric form, Sample Sa.12(1), × 65. From the lower lithunit of the Salima Formation at Bik- faya.

2, 5, 6, 8. Bramkampella atabica REDMOND, l%L Bervtasian.- 2 : Sample Sa. 5(1), × 93 ; 6 : Sample Sa. 12(1), × 34 Axial sectmns and 5 : Sample Sa. 5(1), × 65; 8 : Sample Sa. 5(1)

× 46, equatortal sections. From lowcr hthunlt of Salima For matlon at Bikfaya.

4. Buccicrenata sp. I~almncridgian. - Sample 7N, × 67. An equa torial section from h)wer beds of Bikfaya Formanon at Naas.

7. Trocholina alpina (LEUPOLD, in I,EUPOLD and BIGLER, 1936). Sample Sa. 5(1), × 57. An axml section froln lo,~cr lithuuit of Salima Formation at Bikfaya.


sic se¢hmentation in many areas of the southern Tethys.

The lower carbonates (unit 1) of the Salima For- mation at Bikfaya (Fig. 5) include from 3 m above the base to top of unit an assemblage of Everticy- clammina keller! HENSON, E. contorta REDMOND, Bramkampella arab!ca REDMOND and Trocholina alpina (LEUPOLD). The age assigned to the assemblage is Berriasian. The uppermost carbonates (unit 5) of Salima Formation include another assemblage of Neotrocholina valdensis REICHEL, Riyadhella regularis REDMOND, Riyadhella sp., Trocholina alp!- ha (LEUPOLD) and Everticyclammina keller! HENSON and Nautiloculina oolithica MOHLER. The presence of both Neotrocholina valdensis and Everticyclam- mina keller! in the assemblage dates unit (5) as Ber- riasian-Valanginian in age. Both assemblages in units 1 and 5 categorically date the last phases of carbonate production as Early Cretaceous. Taxa of these assemblages appear along the Mount Lebanon chain, but it is only at the Bikfaya location that the com- plete sequence is preserved.

During Berriasian-Valanginian time, the outer unstable platform in central Lebanon (Salima For- marion) and the inner stable platform in I raq (Zan- gura and Stdaiy Formations), and Saudi Arabia (Bu- waib Formation) were all subjected to shallow marine and evaporite sedimentation. However. during Valanginian - Hauterivian time, the outer unstable shelf in Lebanon was subjected to an influx of fluvio-dehaic deposits whereas the inner stable shelf of h 'aq, I ran, Gulf' States and Saudi Arabia remai- ned exposed to carbonate/evaporite sedimentation. Normal marine carbonate sedimentation resumed over both areas during the Barremian - Apt!an time.

P A L A E O E N V I R O N M E N T S

The larger benthic foraminifera of the Bikfaya Formation occur in various facies, close to or at wave base, in lagoonal settings or in sediments overlying or underlying a massive reef. They lived in shallow water conditions in association with green algae. Where the Bikfaya Formation is preserved, the facies mosaic model of Florida Bay (Laporte, 1967) is rele- vant.

In the Salima Formation at Bikfaya the assemblages of large benthic foraminifera indicate clear, shallow water conditions. The associated grainstone fa- brics indicate high energy, and presence of low angle cross-bedding points to a tidal influence. Such a corn-

bination favours the model of an inner shelU shoreline edge environment of deposition. The shallow water carbonate production was periodically in- terrupted by clay influxes, in the marly intervals and shaley horizons, and occasional extrusions of lava flows. The weathering of lava flows erupted from reactivated older f racture systems generated in the underlying carbonate platform, is the most likely source of clay deposition.

The palaeoenvironmental picture of the uniquely preserved uppermost lithologic units (3, 4 and 5) of the Salima Formation is complex as it shows the first incursion of continental derived detrital quartz sands and the establishment of swampy conditions (lignites) intruding upon an otherwise marine carbonate platform.

C O N C L U S I O N S

The systematic description of larger benthic foraminifera from central Lebanon, collected from continuous sampling of the Bikfaya and Salima Forma- tions, has definitively altered the long-held view of Early Cretaceous deposition coinciding with the advent of the "hasal sandstone". Instead, the transitio- nal Jurassic/Cretaceous time interval is now believed to include the last stages of carhonate production upon a "Late" Kimmerid~an platform within the Bikfaya Formation.

The Berriasian - Valang~nian age of unit 5 (immediately below the "'basal sandstone") of the Salima Formation suggests that, the last phase of uplift and erosion of the carbonate platform coinciding with the elastic continental influx would have occurred during and after Valang~nian time.

Non diagnostic assemblages of larger benthonic foraminifera in the top units of the Bikfaya Formation (top of unit 2 and unit 3) at Bikfaya, and subaerial exposure and erosion of the top lithologies of the Bik- faya Formation at Naas have left the Tithonian ques- tion in central Lebamm unanswered. Similarly, scarce and/or heavily replaced larger benthic foraminifera of the earbonate/evaporites of the inner stable shelf have prevented from the unequivocal recogni- tion of the Tithonian stage within the Late Jurassic sediments. Thus, hostile sechmentary environments for larger tbraminifcra prevailing upon the inner stable shelf, and vertical movements affecting the unstable outer shelf have contributed in obscuring the presence of the Tithonian stage in the region.


The present study draws attention t o / h e presence of Buccicrenata sp. in the lower beds of the Bikfaya Formation and postulates it as a link between Everti- cyclammina and Buccicrenata hedbergi. Descrip- tions of Early Cretaceous forms such as Everticy- clammina kelleri, Bramkampella arabica and Neotrocholina valdensis are made for the first time in Lebanon.

The study also shows that, the position of the Ju- rassic-Cretaceous boundary in Lebanon which was traditionally taken at the lower contact of the "basal sandstone" needs to be revised.

DEDICATION AND ACI/~NOWLEDGEMENTS

The geological field work was carried out by Dr. Germaine Noujaim Clark and the micropalacontolo- gical biostratigraphy by Dr. Marcellc K. Boudagher- Fadel. The authors would like to thank the Lebanon National Council for Scientific Research for its initial financial support.

They dedicate this work to the memory of Dr. Ziad Beydoun, mentor, friend and authority on the geology of the Middle East. His passing away depri- ves the region of scholarship and the best tradition of field and regional geology.

The authors would also like to specially thank Professors F.T.Banner and A. Lord (UCL) who kin- dly reviewed and discussed the earlier drafts of this paper, Mr. D. Clark (Marathon U.K) for their cons- tructive discussions and criticism, and would like to thank the special efforts of Mr.Toby Stiles in the production of the plates.

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the larger benthic f oraminifera and stratigraphy of the upper jurassic/lower cretaceous of central...

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