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New Data on the Lower Cretaceous Microfossil and Nannoconid Stratigraphy in the Guaniguanico Terrane of Western Cuba2 (Figs 1-15)

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New Data on the Lower Cretaceous Microfossil and Nannoconid Stratigraphy in the Guaniguanico Terrane of Western Cuba2 (Figs 1-15) STUDIA GEOLOGICA POLO N I CA Vol. 114, Krakow· 1999, pp. 7- 33. Mesozoic stratigraphy of Cuba Edited by A. Pszczolkowski Andrzej PSZCZOLKOWSKJ1 New data on the Lower Cretaceous microfossil and nannoconid stratigraphy in the Guaniguanico terrane of western Cuba2 (Figs 1-15) Abstract. The age of some Lower Cretaceous lithostratigraphic units and their boundaries in the Guaniguanico terrane, western Cuba, is modified on the basis of calpionellids, forami nifers and nannoconids. In the Northern Rosario belt, the Artemisa/Polier formations boundary is diachronous (upper Lower Berriasian to Lower Valanginian). In the studied sites located in the Southern Rosario belt, the topmost part of the Sumidero Member of the Artemisa Formation is latest Valanginian to Hauterivian in age. Comparing this result with previous data, the Artemisa/Santa Teresa formations boundary ranges from Lower Valanginian to Hauterivian. The Late Valanginian to earliest Hauteri­ vian age of the lowermost part of the Pons Formation in the Rio Las Piedras section, Sierra de los Organos, is accepted on the basis of the planktonic foraminifers, calpionellids and nannoconids. The presence of Tintinnopsella cwpathica Murgeanu et Filipescu is characteristic for the Tintinnopsella Zone. ./llannoconus tru itti i Bronnimann, 195 5, subsp. iruilti iDeres et Acheriteguy, 1980, is present in the Barremian-Lower Aptian assemblages. Comparing the Lower Cretaceous stratigraphic record from the Guaniguanico terrane to that registered at the Southern Gulfof Mexico basin site (Hole 535), some sitnilarities, as well as differences, can be discerned. Key words: Nannoconids, calpionellids, planktonic foraminifers, Lower Cretaceous, stratigraphy, Guaniguanico terrane, western Cuba. INTRODUCTION During the past decades, the Lower Cretaceous formations of the Guaniguanico terrane in western Cuba (Fig. 1) have been studied mostly during the geological mapping (Myc:zyllski, 1977; Pszcz6!kowski, 1978, 1982; de Ia Torre, 1988). These studies allowed to elaborate a general stratigraphic scheme ofth e Mesozoic succes­ sions for the Guaniguanico terrane (Pszcz6lkowski, 1978, 1994). However, various Institute of Geological Sciences, Polish Academy of Sciences, ul. Twarda 5 1/55, 00-818 Warszawa, Poland. 2 Manuscript accepted for publication June 25, 1999. 8 A. PSZCZOLKOWSKI LOWER CRETA CEO US STRA TlGRAPHY 9 define the age of Lower Cretaceous lithostratigraphic units in western Cuba. Pre­ Albian planktonic foraminifers were observed only occasionally in thin sections (de la Torre, 1988), usually without specific identification. The Lower Cretaceous nannofossils have not been investigated in the Gua­ niguanico terrane. Bronnimann (1955) defined the stratigraphic distribution of the species of Nannoconus in central Cuba (former Las Villas Province). Bronnimann (1955) distinguished three typical assemblages ofnannoconids: (1) N. steinmanni­ N. aff. g/obulus- N. colomi, associated with calpionellids, (2) N. steinmanni- N. co­ lomi- N. kamptneri- N. bermudezi- N. globulus (with rare "Globigerinas" in a sin­ gle section), (3) N. truittii- N. minutus - N. elongatus- N. bucheri- N. wassalli, as­ sociated with Orbitolina sp. and with the first "Globigerinas" of an undescribed GOLFO DE type. The age of the assemblage 1 has been determined as the Neocomian, the as­ semblage 2 has been tentatively assigned to the Barremian, while the assemblage 3 BATABANO was defined as Aptian to Albian (Bronnimann, 1955). GEOLOGICAL SETTING 0 40 km The Guaniguanico terrane (lturralde-Vinent, 1994, 1996) consists of a number of tectonic units (thrust sheets) grouped in four belts: the Sierra de los Organos; Fig. 1. L?cation map showing sites sampled in the Guaniguanico terrane, western Cuba (inset Southern Rosario; Northern Rosario; and La Esperanza (Fig. 1). In general, these shows l ocan_o~ of the study area m Cuba). 1- Rio Las Piedras; 2 - San Vicente; 3 - Soroa; 4 _ Rancho Alto; 5-Chmno; 6-:- Ranch? Manetc; 7 - Los Cayos; 8-Lomas de Polier. The site 1 area outlined by belts differ in their stratigraphy and, partly, in their tectonic style (Pszcz6lkowski, the small rectan~le m the S1erra de los Organos belt is enlarged in Figure 2A. The area outlined by 1977, 1978). Nevertheless, the Northern Rosario and La Esperanza belts are similar ~~ger rectangle wlhe northeastern pan ofthe Guaniguanico terrane (dashed line) is enlarged in Figure and may be considered as equivalents. The Guaniguanico thrust sheets were em­ placed northwestvvard during the Early Eocene. The Pinar fault forms the southern boundary of the Guaniguanico terrane (Fig. 1). The Bahia Honda terrane is situated s~ati~aphic problems still remain to be resolved. The pelagic limestones and ra­ to the north of this tectonostratigraphic unit. The Upper Cretaceous and Paleogene dwlanan cherts predominate in the Lower Cretaceous sedimentary sequence of sedimentary sequences of the Bahia Honda terrane are underlain by an ophiolitic western Cuba. These rocks often lack macrofauna, hence the microfossils and nan­ complex and by Cretaceous (pre-Late Campanian) volcanic rocks. The Paleogene nofossils are the main source of biostratigraphic information. Los Palacios basin extends southeast of the Guaniguanico terrane (Fig. 1). The samples were collected at 8 sites in the Guaniguanico terrane of western The Guasasa Formation (Herrera, 1961) has been distinguished in the Sierra de Cuba during 1971-1990. All samples were studied in thin sections for microfossils los Organos belt of the Guaniguanico terrane (Figs 1, 2A). This formation com­ (calpionellids, foraminifers) and microfacies characteristics. The calcareous nan­ prises the ?Upper Oxfordian to Valanginian deposits subdivided into four mem­ nofossils were investigated in the limestone chips on scanning electron microscope bers. The Tumbitas Member consists of thick-bedded calpionellid-radiolarian and (SEM). The principal aims of thi s paper are: (1) to define the age of the lowermost nannoconid limestones of the Upper Berriasian to Lower Valanginian age (Fig. 3). part of the Pons Fonnation in the type section, and to document the lowennost fo­ One sample (AP-20) was taken from the topmost part of the Tumbitas Member raminiferal (planktonic) faunule in the Cuban Lower Cretaceous; (2) to precise the (Fig. 3). Tbe Pons Formation (Hatten, 1957), of the Late Valanginian to Turonian age of the bou~daries between the Artemisa, Potier and Santa Teresa formations; age, also occurs in the Sierra de los Organos belt. This unit, about 150 m in thick­ and (3) to contnbute to the knowledge of the stratigraphic ranoe of the Nannoconus ness, is composed of grey to black micritic limestones with chert intercalations. assemblages in the Caribbean region. o Four samples were collected from the limestones occurring in the lowermost part of the Pons F01mation in the Rio Las Piedras section (Figs 1, 2A, 3). PREVIOUS WORK The Artemisa Formation (Lewis, 1932), recognized in the Southern and North­ ern Rosario belts, is subdivided into three members: San Vicente, La Zarza and Su­ The Lower Cret~ceous ~alpionellids of western Cuba were studied by Pop midero (Pszcz6lkowski, 1978). The Lower Cretaceous Sumidero Member consti­ (1976, 1986). Pszcz6lk:owski (1978) and de Ia Torre (1988) used calpionellids to tutes the upper part of the Artemisa Formation (Fig. 3). This member consists of 11 10 A. PSZCZOLKOWSKI LOWER CRETACEOUS STRATIGRAPHY -r-------- 'crs Gayos Northern • 7 0 Rosario be It ~ . q.'<>~ ~ 6 ------"-~"'~ Ch~rei nos I ' Southern Rancho o Mundito 1000 m F?d}Jl !!mll2 - 3 _ , _4 Fig. 2. A - Detailed location ofthe Rio Las Piedras, southofPons (site I in Fig. 1). 1 - sampled area in the lowem10st pal1 of the Pons Formation; 2 - Guasasa Formation in the Sierra Chichoncs; 3 - roads; 4 - rivers. 8 - Sites 3-8 in Lhe Southern and Northern Rosari o belts (area outlined by dashed rectangle in Fig. I): 3 - Soroa; 4-Rancho Alto; 5-Chirino; 6-Rancho Mancte: 7-Los Cayos; 8 - Lomas de Polier biomicrites with intercalations of radiolarian cherts. The samples of the Sumidero Member limestones were collected at four sites (Fig. 1): Soroa; Rancho Alto; Chir­ ino; and on the Rancho Manete hill. The Potier Formation (Pszcz6lkowski, 1978) I occurs in the Northern Rosario belt. This formation, about 300m thick, includes pe­ lagic limestones with intercalations of turbiditic sandstones and shales. The Roble l z Member was distinguished in the uppermost part of the Polier Formation. Three => s samples were collected from the topmost beds of the Potier Formation (Figs 1, 2B, "' c 3~ 0 z;.." j Uz 8 0 Oo ~ u 3). ; D ~N z z ... DESCRIPTION OF SAMPLED SITES oil ;;; j - $ g. h tj"' ~w 1S,. ! ~~ .. l! Sierra de los Organos belt ;; ~ &E ~ii ~ i~ D V 2 1~ X <) x - i Rio Las Piedras (Fig. I: site 1) I This site is located south ofPons (Fig. 2A) in the type section ofthe Pons Forma­ I I tion (Hatten, 1957). This formation consists ofpelagic limestones interbedded with I I cherts. Their age was originally considered to be Albian to Turonian (Hatten, 1957; I Khudoley & Meyerhoff, 1971). Later, the age ofthe lowermost part ofthe Pons For­ I I mation was defined as ?Hauterivian (Pszcz6lkowski, 1978; de Ia Torre, 1988). The Joddn JSMOl •addn JIVI\Cl s:mns JaMCl I NVII"l3~~ve I N't'IAI~3J.n'<' H I N\fiN I ~NVl'o'A N'o'I S\fl~~38 Pons Formation occurs in the lowermost tectonic units of the Sierra de los Organos N'o'IJ.d'o'l belt, only. In the Rio Las Piedras section, the Pons Formation consists ofgrey bedded lime­ stones with occasional chert intercalations, lenses or nodules. The contact of the Pons Formation with the underlying Guasasa Formation (Fig. 3) is not exposed in this section. Four samples collected from the limestones occurring in the lowermost 12 A. PSZCZOtKOWSKI LOWER CRETACEOUS STRATIGRAPHY 13 (f) rite, that it was not possible to obtain light micrographs of 0 NANNOFOSSILS z -()~w - >- (f) ..J good quality. For this reason, computer drawing was made 0 (.9 Z LL ..J (/) (/) (f.) (f.) i= w 0- ::J ·- ::;:, ::;:, ::;:, ·- from a micrograph (Fig.
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