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刀 by F ritz E Steininger, M . P A ubry, W A . B erggren, M . B iolzi, A . M . B orsetti, Julie E . C artlidge, E C ati, R. C orfi eld, R . G elati, S. 1accarino, C . N apoleone, E O tm er, F R6gl, R . R oetzel, S. Spezzqferri, F Tateo, G . Villa, D . Zevenboom The G lobal Stratotype Section and Point (G SSP) for the base of the N eogene The P aleogene-N eogene P eriod-孙stem boundary, L ocal position: 35 rn from the top of the Lem m e- C af osio Section. w hich defines also the O ligocene-M iocene Ep och Sedim entological m arker: A n excellent lithological m arker for the G SSP is provided by a distinct boundary betw een lithologic U nit A -Series boundary is defi ned in the L em m e-C arrosio (the m ore m assive part of the section) and the overlying lithologic section in the village of C arrosio, south of the tow n of U nit B - I (the m ore stratified part of the section) A t the 50 im m ark, G avi and north of Voltaggio 沮lessandria P rovince), there is a horizon w ith yellow ish nodules. T he G SSP is exactly 15 m etres above this lithologic boundary. A layer w ith yellow ish nod- northern Italy. ules lies in lithologic Subunit B 2, exactly one m etre below m etre 35 (Figure 3). A rtificial m arks: The top oft he section (0 m ) corresponds to the top H istorical background and concepts of the R igoroso Form ation. For practical reasons, a m etal stake w as not placed at level 0 but exactly 0.50 m below the top of the form a- T he historical background of the concepts of 'stratigraphic units' of tio n. A steel cable run s fro m th e 0 m m ark to th e b ase o f th e sectio n . L yell （1833) and of M . 1-16m es (1853) (the C hronostratigraphic E ach m etre of the section is m arked by a m etal tag (w ith the m etre U nits of m odem usage) have been based m ainly on tw o observa- num ber). These tags are fixed at the cable and additionally in the for- tions: (1) m ajor or m inor discontinuities (or facies changes) in rock sequences and (2) m ajor or m inor changes in the overall biotic con- I U G S ！C S tent, or w ithin a specific taxonom ic group. M . M im es (1853) defined G S S P the N eogene using both characteristics. In his w ork published in P A L A E O G E N E 1853 (p. 806) H 6m es discussed his 'organic' (paleontologic) reasons N E O G E N E B O U N D A R Y for com bining Lyell's (1833) M iocene and Pliocene into his N eo- A T M E T E R 3 5 gene by referring to the m ollusc fauna: 'die Verschiedenheit der ('of 1 9 9 3 the m ollusc') Fauna der Eoedn- und M iocdn-Epoche' of L yell and m ation. In addition m etre 35 is m arked by a m etal plaque fixed in the in 1864 (p. 510) he pointed out the widespread discontinuities: section w ith the follow ing text. 'Unstreitig haben zw ischen der E ocen- und N eogenzeit gew altige The section has excellent e x p o sure, absence of m ajor structural Schichtstdrungen in Europa stattgefunden'. com plications and apparent absence of unconform ities w ithin the so called 'critical tim e span'. In addition, there is an adequate thickness C oncepts of th e W orking G roup of sedim ents, favorable facies, rather good potential for planktonic The base of the N eogene System and the base of the M iocene Series m ust be situated betw een the C hattian and A quitam an Stages, so that the A quitanian Stage is included in the N eogene System . T he Paleo- gene-N eogene System B oundary coincides w ith the O ligocene-M iocene Series B oundary. T he ideal G SSP candidate for the P aleogene-N eogene System boundary w ould be a tem porally r旧 n a continuous section representing the so called 'critical tim e span'. C. Campagnola This 'critical tim e span' w as determ ined to be represented by the 么 R ic o i biostratigraphic interval betw een planktonic foram iniferal Z ones P21 to M 2 of B erggren et al. (1995). In term s of calcareous nanno- 、， \\'I-. fossil zonation it corresponds to the interval from Zone N P25 t t ，，‘，气 (Sp enolithus ciperoensis Zone) to Z one N N 2 (D iscoaster druggi C am poreg 0 鱿 、、、 Zone) as defined by M artini (197 1) and M artini and M oller (1986). 日erg am o ；(.}arezzanIi M ILA N O N o v a ra 10 产一 M ain features of the proposed G SSP R oc ch e tta 乙anavila R iver N am e: B ase of the N eogene System (base of the M iocene Series, A lessandrra Paleogene-N eogene System boundary and O ligocene- M iocene Series boundary). 口 袱 R ank of the boundary: System (beginning of the N eogene Period) 协 梦飞、 L ocality nam e of the G SSP : L em m e-C arrosio section, Italy 嘛 G eographic position : L ongitude 8'50'11" E ; Latitude: 44'39'32' G E N 半 N . Carta G eologica d'Italia: Foglio G EN OV A N o. 82 (1: 100 000); T av. V O LT A G G IO I N E (I：25 000) (Figure 1) F igure I G eograp hic location of t he L em m e-C arrosio section. Episodes, Vol. 20, no.］ 2 4 and benthic m icrofossil biostratig raphi e s, m agnetostratigraphy, sta- form ed by Perm idic and L igurian tectonic units. T he late E ocene to ble isotope stratigraphy and, eventually cyclostratigraphy. late M iocene succession form s a large hom ocline, gently dipping to T he section is easily accessible by public and priv at e trans- the northw est. T he basin form ed during the late E ocene--early portation and the present ow ner of the property M r. N ando T raverso O ligocene as an extensional basin behind the arc of the W estern has agreed to provide access to colleagues interested in visiting and A lps. It w as affected by the A pennine com pression from late sam pling the section and to conserve the section as an international O ligocene. E vidence ot post late M iocene extensional tectonics are geological point of prim e interest. clearly recorded (Falletti et aL 1994). The facies evolution of the Piedm ont T ertiary B asin is strongly controlled by synsedim entary G eology of the G SSP site tectonic activity and three large-scale facies belts can be recognized. From w est to east: the Langhe-, the V isone-L ernm e- and the Bor- T he are a of the L em m e-C a rro sio section is situ ated w ith in th e P ie d- b era- S taffo ra facie s be lts. T he G S SP sectio n is situated w ithin th e m ont T ertiary B asin, in southern Piedm ont, northw estern Italy (Fig- V isone-L em m e facies belt in the upper part ot the R igoroso Form a- ure 2). T he basin itself is bordered by the arc of the W estern A lps and tion w hich overlies the M olare Form ation (O ligocene fan delta con- by the northw estern end of the N orthern A pennines. Its basem ent is glom erates w ith sandy shallow m arine intercalations yielding m icro- 口 回 姗 皿 黝1 既 塑 黔吕 圈 寨 粼REA 勺 7 藕 厂 V E N E Z IA 干0 一 裹 MILGAENOVA 一” 一 1 P_' _ 一 却 V E R C E L L I o FIR EN ZE 多经． 一 1 ？ 0}} ＿＿关产减沁火 尸 P A V IA O ， 粉篆热 闷 飞 0 、、、 TO RIN O O C A S A LE 瘾童鳌肇缪麟 M O N F E R R A 蒸曰沼豁 1}1笋气CHIERI F,J0 .-4 ". '4%, - 1, -1 7}- 'I} V O G H ER A 0 1 41} 、、 、、 篡 A L ES SA N O AS0TI 群娜尧 巍琴寒橇粼 舜补盆蔑之阅 王口 0 PINERCLO丫 Y v 魏 勺‘ 、 T 类 % 荞 。：。 朴 l茱 燕 薯SALUZZOF O S S A N O 戮.......E.M .I.LIA 魏 嘿 匕 鞭 S v 0 C U N EO N 黝之 ＿0 GE N OVA 一 妇 杂 S A V O N A 0 5 10 k m 1 ． I F igure 2 The geologicf ram e of t he P iedm ont Tertiary B asin. L 6 S Location of the Langluan type section. Upper Eocene to lower Oligocene deposits: 9 Depo-center axis of the Plio-Q uaiernary b a sins . T Location of the Serravallian type section a alluvial to coastal conglom erates, shallow- 10 B u rie d th ru st fro n t o f th e C o llin a d i T o rin o - I Location of the Tortonian type section.
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  • The Phylogenetic and Palaeographic Evolution of the Miogypsinid Larger Benthic Foraminifera

    The Phylogenetic and Palaeographic Evolution of the Miogypsinid Larger Benthic Foraminifera

    The phylogenetic and palaeographic evolution of the miogypsinid larger benthic foraminifera MARCELLE K. BOUDAGHER-FADEL AND G. DAVID PRICE Department of Earth Sciences, University College London, Gower Street, London, WC1E 6BT, UK Abstract One of the notable features of the Oligocene oceans was the appearance in Tethys of American lineages of larger benthic foraminifera, including the miogypsinids. They were reef-forming, and became very widespread and diverse, and so they play an important role in defining the Late Paleogene and Early Neogene biostratigraphy of the carbonates of the Mediterranean and the Indo-Pacific Tethyan sub-provinces. Until now, however, it has not been possible to develop an effective global view of the evolution of the miogypsinids, as the descriptions of specimens from Africa were rudimentary, and the stratigraphic ranges of genera of Tethyan forms appear to be highly dependent on palaeography. Here we present descriptions of new samples from offshore South Africa, and from outcrops in Corsica, Cyprus, Syria and Sumatra, which enable a systematic and biostratigraphic comparison of the miogypsinids from the Tethyan sub-provinces of the Mediterranean-West Africa and the Indo-Pacific, and for the first time from South Africa, which we show forms a distinct bio- province. The 116 specimens illustrated include 7 new species from the Far East, Neorotalia tethyana, Miogypsinella bornea, Miogypsina subiensis, M. niasiensis, M. regularia, M. samuelia, Miolepidocyclina banneri, 1 new species from Cyprus, Miogypsinella cyprea and 4 new species from South Africa, Miogypsina mcmillania, M. africana, M. ianmacmilliana, M. southernia. We infer that sea level, tectonic and climatic changes determined and constrained in turn the palaeogeographic distribution, evolution and eventual extinctions of the miogypsinid.