http://dx.doi.org/10.18268/BSGM2019v71n3a5 P. 691‒725 VOL. 71NO. 3 BOL. SOC.GEOL.MEX.2019 Coyoacan, 04510,CDMX,Mexico. Autonoma de Mexico, Ciudad Universitaria, Facultad de Ciencias, Universidad Nacional Iriliana López-Caballero Potosi, Mexico. Potosi,Luis San de Av. Dr. Nava Luis San 5, # Instituto de Geologia, Universidad Autonoma José RamónTorres Rubén López-Doncel 04510, CDMX,Mexico. de Mexico, Ciudad Universitaria, Coyoacan, Geologia, UniversidadNacional Autonoma de Paleontologia,Departamento Instituto de lomanya@geología.unam.mx Gloria Alencaster Lourdes Omaña Iriliana Lourdes Taxonomy, biostratigraphyandpaleoenvironmentalimplications Formation WValles-SanLuisPotosiPlatform,central–easternMexico: Mid–late CenomanianlargerbenthicforaminifersfromtheElAbra Manuscript May accepted: 11,2018. Corrected manuscript received: May 7,2018. Manuscript received: 5,2018. April López-Caballero Omaña , Rubén López-Doncel Mexico. Formation, San Luis Potosí, thic foraminifers,El Abra Keywords: Cenomanian, ben drowning. duringtheplatform deposited and pithonellids and the occurrence of of with anacme wackestone–packstone of microfacies (Soyatal Formation) consists turea wackestone–packstone. is Another abundant miliolidsandostreids. tex The Abra Facies) can bededuced from the wackestone. Arestricted environment (El packstone–grainstone, andpackstone– includes peloidal-foraminiferal packstone, (Taninuldeposit Facies) is inferred. It shallow-water, open marine platform Taninul andthe El AbraFacies. Awarm, recognized in the El AbraFormation: the correlativegraphically facies have been cretacea planktic foraminifera ( dant pithonellidsand Soyatal Formation, which containsabun the input from of the hemipelagic deposit changes andanincrease in siliciclastic demise is coincident with major sea-level disappears. benthicforaminiferal The miniferal assemblage is reduced and later the fora where the species richnessof by the foraminiferal association.overlain It is characterized by anabundant benthic Zone. Assemblage first Zone is The Zone and posed thesefindings, two zonesare pro of basis dated as mid–late Cenomanian. On the theElAbraFormation were upper part of paper. fromstudied successions The the which are described and illustrated in this iferal assemblage that includes 18species, it contains abenthic foramindeposit; ashallow-water Formation of consists through Upper Cretaceous. El Abra The Mexico duringthe middle (Albian) of thatsystem rimmed the ancestral Gulf an extensive carbonate platform part of Valles–SanThe Potosí Luis is Platform ABSTRACT , José r-k Partial Range Zone).Two strati Nezzazatinella picardi Pseudolituonella reicheli strategist foraminifersplanktic Ramón TorresRamón Nezzazatinella picardi Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín r Whiteinella archaeo Whiteinella and Interval Zone Assemblage r-k strategist , Gloria Interval ------r

Alencaster que incluye 18especies, quesedescriben ilustrane de foraminíferosconjunto contiene un bentónicos poco profundas; ésta de aguas Abra es un depósito Albiano hasta el Cretácico Superior. La caliza El traba bordeando el antiguoGolfoel deMéxicoen queseencon extenso sistemaun deplataformas Valles–SanLa Plataforma Luis Potosí es parte de RESUMEN Potosí, México. ElAbra, San Luis Formación foraminíferos bentónicos, Palabras clave: Cenomaniano, (Formación Soyatal). sitados durante la inundación de la plataforma sencia de foraminíferos r y r-k depo de estrategia packstone con unaugede pithonélidos y la pre Otra microfacies consiste de un wackestone- textura dela rocawackestone-packstone. es un por los abundantes miliólidos y ostreídos. La restringido (Facies El Abra) puedededucirse packstone ypackstone-wackestone.ambiente Un incluye unpackstone peloidal con foraminíferos, cálidas someras (Faciesaguas Taninul). Ésta marina abierta de de plataforma un depósito Facies Taninul yla Facies El Abra. Se infiere han sidoreconocidas en la Formación El Abra: la correlacionablesDos facies estratigráficamente Alcance Parcial archaeocretacea)). (Whiteinella feros ryr-k(Zona de planctónicos de estrategía que contiene abundantes pithonélidos y foraminí hemipelágico de la Formación Soyatalel depósito de sedimentos desde mar y un aumento en el aporte del cambios de nivel es coincidente con grandes rece. deforaminíferos La desaparición bentónicos las asociaciones de foraminíferos desapa y luego picardi donde se reduce la riqueza deespecies de Nezzazatinella cida por la Zona de Intervalo dante de foraminíferos bentónicos. Está sobreya Conjunto secaracteriza por una asociación abun Nezzazatinella picardi). La primera Zona de Pseudolituonella reicheli y Zona de Intervalo tardío; se proponen dos zonas (Zona de Conjunto fueron datadas como del Cenomaniano medio– la parte superior de la Formación de ElAbra en este documento. Las sucesiones estudiadas de , /2019 691 ------

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation ABSTRACT Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation INTRODUCTION 692 692 1. Introduction et fthe Tethys (Schroederments of and Neumann, the tropical–subtropical shallow-water environ developmentate platform took place throughout Albian through Cenomanian,widespread carbon During the mid–Cretaceous, particularly inthe soeli yasceso fbioclastic packstone is overlain byof asuccession val (Basañez ing at the Cenomanian/Turonian inter boundary precedingdeposit the VSLPP, which wasdrown studyrepresents the lastshallow-water area of the El AbraFormation inthe upper part of The orbitolinids(Omaña mostly of part composed the eastern iferal association of and is very different from the well-known foramin ation has been dated as middle-late Cenomanian the VSLPP.from part of associ the western This We studiedthebenthicforaminiferal community schlumbergeri Pseudonummoloculina heimi nutensis of VSLPP. They reported an assemblage composed Tavitas part andSolano (1984) from the eastern Formation were documented by Bonet (1956), and Albian benthic foraminifers fromThe the El Abra and García-Barrera, 2008). 1973;Alencáster,1930; Coogan; 1998;Alencáster been analyzed by numerous ( authors brate fossils, primarilyAlbianrudists, whichhave El Abra FormationThe is renowned for its inverte algae, corals, andannelids. echinoderms, thic foraminiferal assemblage that alsoincludes containing anabundant andwell-preserved ben derived from the Cenomanian ElAbra Formation In thisstudy, we analyzed calcareous samples contained intheElAbraLimestone. and diverse benthicforaminiferal assemblage now arich experienced the evolutionplatform This of Mexico (Salvador, 1991). of the ancestral Gulf systemthat awide carbonate bordered platform of Valles–San PotosíLuis (VSLPP) part was Platform In Mexico, duringthe Albian/Cenomanian, the most important groups that inhabited this milieu. 1985, p. 5). Benthic foraminifers and algae are the / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Orbitolina (Mesorbitolina) texana, DictyoconusOrbitolina (Mesorbitolina) texana, wal (Carsey), (Munier-Chalmas). etal Coskinolina sunnilandensis ., 1993;Omaña (Bonet), and et al etal. ., 2016). e.g. , 2012).It (Maync), Adkins, Dicyclina ------/2019 rudists andlarger benthicforaminifera. as such organisms benthic affected that change nella archaeocretacea occurred during the latest Cenomanian ( the carbonate platforms the demise of start of The Korbar 1997; Hart (Drzewiecki andSimó, 1977; Caus forms plat Mediterranean of flooding widespread and Hallam, 1992; Miller with risingsea level (Haq nian (C/T) interval at level the global is linked drownedThe the Cenomanian/Turo in episode andpithonellids(Soyatalfers Formation). and pelagic wackestonebearing planktic foramini pithonellids, and intervalthis overlain is by withabundanta deposit chrysalidina, Later, such as onlyforms Merlingina, Hemicyclammina, Dicyclina, and Cuneolina as such forms larger of first interval is characterized by the disappearance However, inthe present study, the C/T boundary larger foraminifera.” extinctionsecond step of themesotrophicthreshold triggered the the riseof tunist planktic foraminifers predominated while when the high productivity only persisted Pseudolituonella Chrysalidina, largersuch foraminifera as to lesscomplex forms extreme most the alveolinids, the eliminated step first “the (Italy). They stated Apennines that the southern of upper Cenomanian in shallow-water carbonates largerthe in foraminifers extinction of of ttern Parente thic foraminifera at theC/T boundary. ben the affected extinction major a when occurs textularids, and trochamminids. step Atsecond werenifera scarce poorlyand diversified miliolids, Cenomanian ( at the top of Pseudocyclammina in twothe genera steps; mented that the benthic foraminifera were affected Philip and Airaud-Crumière (1991, p. 117)docu et al. et al. k srtgss euigtedvriyo the strategists, reducing the diversityof rotalids, miliolids, remained, and algae etal. , 2012). (2008) also reported a two-step pa Geslinianum Juddii , and 20; El-Sabbagh 2005; , r Zone),withamajorbiological and Zone) the benthic forami et al. Pseudolituonella r-k Nezzazatinella picardi, Prae Praealveolina, Chrysalidina, Praealveolina, Chrysalidina, , 2005; Gale Zone. During the late strategist planktic fora et al. and Pseudolituonella, Daxia, , 1987;Haq,2014; Pseudoraphydionina disappeared etal. et al r ., 2008), –oppor , 2011; Whitei et al., ------. ;

biostratigraphic standardsbiostratigraphic based onthem in the the benthic foraminifers, comparingthe value of theage the El Abra Formation using the stratigraphic of c) toconstrain the VSLPP; of flooding foraminifersbefore their demise, causedbythe the larger about the distributioninformation of theTethysRealm; part of western b)toprovide the this unit in Mexico andof assemblage of the faunal as acontribution tothe knowledge of the El Abra Formation from the upper part of identified foraminifers benthic the illustrate and the workare a)todescribe objectivesThe of theplatform. floodingof a result of gella, Heterohelix, Globigerinelloides suchwith simplemorphologies, as minifers Figure 1 Mapwithlocationsof theanalyzed sections. , and Whiteinella Whiteinella Hedber Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín as - 2. Geologicalsetting nteGl o Mexico Basin.Duringthis period, of in the Gulf stability tectonic significant of time a was taceous ico. According to Salvador (1991), the Early Cre Mex of the Gulf association with the opening of theVSLPP,part of in whichthe western formed San Luis Potosí (Figurearea 1). This belongs to the city of samples wereThe collected east of aboutthepaleoenvironment.information foraminifers andthe microfacies study to infer the larger the paleoecological dataintegrate of the overlying unit;andd)to the planktic age of peri-Tethyan area; moreover, supporting itfrom /2019 693 693 - -

INTRODUCTION / GEOLOGICAL Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation SETTING GEOLOGICAL SETTING / MATERIALS / Mid late Cenomanian larger benthic foraminifers from the El Abra Formation – RESULTS 694 694 i fthe Gulf, acrossMexico to the Yucatanrim of extended from the Bahamas along the northern during the Albian, when carbonate deposition widespread carbonate particularly deposition, of the basin became the site central part of the deep the stable shelves, ramps, bordering andplatforms and decreased sediment terrigenous of influx the (1993), Aguayo (1998),andLópez-Doncel (2003). processhas been recorded by and Stephens Enos and Torres-Hernández depositional (1994).The (1990), Basañez (1993), Wilson and Ward (1993), (1963), Carrillo-Bravolo-Barradas (1971),Suter VSLPP been described has by andBel Cserna Luis Potosí. framework stratigraphic The for the San the city of seen along roadeast of cuts30km Potosí– Luis sidecanbe itswestern San Tampico railway). Part of the of 541–546 (km Morelos the Cuesta de El Abra near Valles and Antiguo margin isexposed along inquarries shelf eastern Oriental fold-thrust belt (Suter, 1984;1987). Its VSLPP now MadreThe lies within the Sierra Mexico. of the Gulf margin occuringat sametime as the opening of paleo-Pacific the from deposit a as authors these Río Verde,Potosí. SanLuis byinterpreted Itis detrital zircon from the El Alamito locality at W that the VSLPP overlies Toarcian rocksdated by Recently, Venegas-Rodríguez between Nuevo LeónandTamaulipas”. Ciudad Victoria on the state line km southwest of Paleozoic schist that is exposed at Miquihuana, 70 anorth-northwest–trending Precambrian gneiss andUpper tectonic ridge of of flank western along the south apparently formed platform The margin. Albian, when itevolved arimmedshelf Cretaceous, but reached itsmaximum area in the Mexico. It initiated in the Early of the Gulf side of (200 by platforms 300km)located on the western “thelargest isolated carbonate VSLPP is oneof Wilson andWard (1993,p. 42)stated that the 2), which remained active untiltheCenomanian. more locally restricted, such asthe VSLPP (Figure in east-central Mexico, were carbonate platforms the basin (Scott, 1990). Along the flankwestern of Peninsula, andto various Caribbean localities / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín et al. (2009) stated - - /2019 3. MaterialsandMethods 4.1.2.1. LLANODELCARMENSECTION (LLC) 4.1.2. THETANINUL FACIES 4.1. LITHOFACIES ANDMICROFACIES 4. ResultsandDiscussion mitted precise identification; the biostratigraphic biostratigraphic the identification; precise mitted faunalpreservationtion. The good, which is per tion for foraminiferal and microfacies examina stratifica the to perpendicular and parallel both 5 to 10 m. The 150 thin of sections were prepared samples wereThe collected at an average interval the LaMinitaoutcrop (LM). (C), El Temazcal(G), Cerritos (ET), as well as in (LLC), Guadalcázar VSLPP: Llano del Carmen the located100 mthick part of at the western lected from fourthat sections ranged from 40to the El Abra Limestone (Figure 2). It was col of studiedmaterialThe fromcomes the upper part mation andis~100mthick(Figure 4). the El AbraFor massive dark-gray limestone of of consists It 100°40ʹW). 22º45ʹN, (coordinates SanLuisPotosí the city of cropsout north of section (LLC) currently Llano del Carmen The and describedfrom theTaninul facies. followingThe weresections measured, sampled, (Figure 3eand3f). limestone rich light gray miliolids andostreidsin (Figure ElAbrafaciesisa algae 3a to 3c). The rudists, foraminifers and mostly composedof is athickto massive skeletal bioclastic limestone correlated (Aguayo, Taninul 1998). The facies Taninul andElAbra,which are stratigraphically El Abra FormationThe displaystwo facies, the the paleoenvironment. microfacies study out to reconstruct was carried foraminiferal ranges. stratigraphic Inaddition,a schemebased onthe benthic andplanktic is - - - - - Figure 2 101° 00´ are embedded in microsparitic cement, densely the content can be recognized. They 60% of tum Bouenia Peneroplis parvus, Nezzazatinellasimplex, picardi, Spiroloculina cenomana, N. Nezzazata gyra, Cuneolina parva, Cuneolina pavonia, cretacea, Pseudocyclammina Daxia cenomana, Hemicyclammina sigali, Merlingina species richness that includes with highforaminiferal packstone–grainstone petrographicindicates analysis The apeloidal SAN LUIS POTOSI aepeet h opnnso more than are present. components of The Geologicalmapshowing theElAbraand SoyatalFormations(modified fromLabarthe sp. andencrusting and ioxa inflata Minouxia sp. , Dicyclina schlumbergeri, LA MINITA Pseudolituonella reicheli, Lithocodium LLANO DEL CARMEN VILLA HIDALGO . The algae algae . The

aggrega Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín - GUADALCAZAR 101° 30´ CERRITOS EL TEMAXCAL miliolids and other forms such as miliolids and other forms of consisting sorted foraminiferal grainstone a coated, poorly Other microfaciesof consist this association. note that rudist significant restriction in water circulation. to important Itis to subjected not platform open rine assemblage indicatesa normal-ma in adeposit environment. and faunal–algal lithology The moderate transport into a relatively high-energy arecomponents coated with micrite, suggesting the a matrix-supportedpacked in of fabric.Most 22° 30´ 22° 00´ Hippurites resectus 0 et al. MAASTRICHTIAN PLEISTOCEN TURONIAN CONACIAN OLIGOCEN MIOCEN CAMPANIAN SANTONIAN APTIAN HOLOCEN PLIOCEN EOCEN CENOMANIAN PALEOCEN ALBIAN 5 , 1982;López-Doncel, 2003). Se E cal 1 E km 0 E E Villages E E Thrust C Recumbent Studied sections Studied way Free Anticlin Anticlin E ity Andesite Basalt Cura del Cuesta La Peña La LITHOLOGY crater explosion and Basanite 520 15 isalsofound in /2019 Cárdenas Peneroplis parvus Soyatal e e Abra Alluvion Rhyolite El Conglomerate cama Guax- Tama- Granite bra 695 695 - ,

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 696 696 4.1.2.2. THEGUADALCÁZAR SECTION(G) -LM-1); f: Benthic foraminiferal-LM-1); f:Benthic wackstone–packstone(SampleLM-5). abundanceC-10); e:Wackestone–packstonewithagreat of miliolidsand thin-shelled ostreidsoriented inaparallelarrangement (Sample Calcisphere-richpackstone-wackestone (Sample d: C-9); packstone (Sample Worn algal c: LLC-4); (Sample miliolids classifiedwith poorly Figure 3 city of San Luis Potosí (22°64ʹN, 100°38ʹW). The The Potosí(22°64ʹN,100°38ʹW). Luis San of city the Guadalcázar section(G) is locatedThe NE of micritized (Figure 3b). andmicrofossils the grains and algae; are strongly / Microfacies oftheupper partoftheElAbraFormation.Scalebars100µm.a:Packstone–grainstone(SampleET-2);b:Grainstone Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín /2019 subordinate with the same foramin grainstone and packstone bydominated is lithofacies The 5). Taninulthe Facies (Figure of thick m ~50 deposit calcareous a gray los García stream. of It consists El Abra Formation that crops out in the Aguaje de the belongs to studied the succession upper part of - 4.1.2.3. THECERRITOS SECTION(C) Luis Potosí–CerritosLuis road(22°43ʹN, It 100°28ʹW). section (C) was measured Cerritos on the San The the Soyatal Formation, which here is 15mthick. overlainEl Abra limestone is unconformably by (Wilson, 1975) in the (open platform marine). The Facies Zone 7 to 8 2004) of (SMF) 18 (Flügel, as Standard Microfaciesfacies is interpreted Type site.micro facies asat This the Llano del Carmen increase inpractically the same micro in energy sparitic cement represents an presenceThe of Clypeina containing algae, such as sitebut iferal assemblagethe Llano del as Carmen sp. Figure 4 Salpingoporella hasi Llano delCarmensection. LLC-10 LLC-7 LLC-1 LLC-9 LLC-6 LLC-5 LLC-4 LLC-8 LLC-2 0 SCALE 10m and Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín - - 2004). foraminifera (Flügel, or calcareous algae” green with abundant andpackstones grainstones benthic type couldbecomparable toSMF18“bioclastic anoriginal micriticmatrix. microfacies The of cement, mass,shows smallremains mostlysparry ground fabric. The a grain-supported forming 50%, exceeds locally components of percentage rich inpellets and pseudopellets.grainstone The Microfacies 1–Benthicforaminiferal packstone– lowing 2microfacies: In the El AbraFormation we recognized the fol the Soyatal Formation (Figure 6). Taninul Facies, overlain andit is conformably by the the El Abra Formation of the upper part of from limestone gray massive of m 45 of consists /2019 697 697 - -

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 698 698 Figure 5 0 m 0 ronments, and avariationthe water in can energy transported from to low-energy envi high-energy been have components main The 1975). (Wilson Facies Zone7of environment of an openseashelf microfaciesThis issimilarto SMF10,suggesting could be related to an increase in nutrient supply. tinella picardi of community reducedis tosmallforms (Figure algae 3c). amount of matrixfine-grained containing a larger embedded Microfacies 2–Worn packstone,algal a within the seawater.conditions, andgoodoxygenation of salinity,zoneswith normal stable temperature blage indicates precipitation inshallow subtidal assem fossil The Wilson(1975). of 7 FaciesZone to corresponding open marine interior platform, wavenormal base, withinthe euphotic zone inthe ashallow marine suggests environment above the thismicrofacies environment depositional The of / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Guadalcazarsection. 5m G-6a G-6 G-4 G-5 G-7 G-8 G-2 G-1 G-3 ? ? ? ? ? ? ? ? ? ? , miliolids, and rotalids.change This The foraminiferalThe Nezazza - - - /2019 4.1.2.4. THEELTEMAZCALSECTION (ET) lids, fabric. In addition to the pithonel grain-supported to mud a in components the of 50% than more pithonellids can be up to population3d). The of variesmicrosparitic locallyin cement(Figure pithonellids embedded in amicriticmatrix that stone, thismicrofaciesa bloom contains of Microfacies 3–Pithonellid-rich packstone–wacke tion represented by thenext microfacies: the hemipelagic–pelagic Soyatal Forma stone of changes to marlyUp-section, the lithology lime openmarineenvironment).platform, microfaciesto Facies corresponds Zone7(interior (microsparite). clasts andgroundmassgrains This thebio be inferred fromthe increase size in of shale unit. capped byunconformably a reddish calcareous corresponding tothe El AbraFormation, andis is It gray, massive limestone of 40m 100°50ʹW). of composed (22°38ʹN, locality Quemado analyzedThe section was measured in the Cerro event. aninitialdrowning certainly evidencement is of environ depositional its but shelf), (deep (1975) Wilson foraminifers) anda Facies Zone2to 3 of (wackestone to packstone with pithonellids and (2004) be similar to types SMF2and3Flügel the micritic groundmass.microfacies This could microfauna in bles anunsorted accumulation of recognizable;the components is rather, itresem of orientation or microlamination No identified. sp., Small benthic foraminifera r/k connect the environments, as andmorphotypes potential and are adapted to eutrophic or unstable that havesimple morphologies high reproductive tests and um-sized species withunornamented W. paradubia. cea, W. archaeocretaMacroglobigerinelloides Whiteinella caseyi, M. planispira, Heterohelix moremani, Heterohelix reussi, also present, including -intermediate species (Gebhardt -intermediate Lingulogavelinella r and cf. W. W. aprica, baltica, W. brittonensis, r-k r The The and strategist planktic foraminifera are k r morphogroups and are called morphogroups -strategists are smalltomedi sp., androveacrinids were Muricohedbergella delrioensis,Muricohedbergella Dorothia Whiteinella Whiteinella sp., et al Gavelinella ., 2010). that and ------

4.1.3.1. THELAMINITA OUTCROP (LM) 4.1.3. THEELABRAFACIES El Abrafacies (Figure 7). the cream limestone of to light-gray 8 samplesof At this locality (22°78 5ʹN, 100°85ʹW), we collected 2004;Wilson,1975).7 (Flügel, ties, which includeSMF8to 10 inthe Facies Zone facies zone are similarto those at the other locali is present. standard The microfacies type and the the other sections, but the algae of foraminiferalfabric. The association is like that atypicalgrain-supported exceeds 60%,forming texturegrainstone and locallythe component limestone inthislocalityhaspackstone– The Figure 6 Cerritos section.

Ce-14 Ce-15 Ce-12 Ce-17 Ce-13 Ce-1 Ce-16 Ce-11 Ce-10 Ce-8 Ce-3 Ce-7 Ce-2 Ce-6 Ce-4 Ce-9 Ce-5 0 m 0 Neomeris cretacea 10m Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín - aktn–aktn ihahge iest fwith ahigher diversitywackstone–packstone of 2) another that showsa benthicforaminifer-rich Facies and Zone 7 inthe interior platform; of 2004) istics are comparable to SMF 8(Flügel, with amud-supported character fabric. These components are embedded in amicriticmatrix ment points to some control by the current. The shallow-watersuggests settings and the arrange benthicforaminifera (Figure presence 3e). The of whichare well-oriented a parallel in arrangement miliolidsandthin-shelled ostreids, abundance of stone–packstone withreduced diversitybut agreat awacke 1) defined: are microfacies Two thick). the El Abrafacies(40m cream limestone of of LaMinitaoutcropThe displaysseveral examples /2019 699 699 - - -

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 700 700 4.2. AGE Figure 7 and Neumann, 1985). and planktic foraminifera are absent (Schroeder fossilswhen other fossilssuch as the ammonites ments, where theyare the most prominent marker environ shallow-water in significant graphically Cretaceous larger benthic foraminifera are strati withmoderate energy.platform Facies Zone 7 intheinterior as SMF10to11of microfacies.first This microfacies can be classified in comparisonwiththe denser (grain-supported) micritic upto microsparitic andthe fabric ismuch pavonia olina maccagnoae, Dicyclina schlumbergeri, species including / Temazcalsection. Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín (Figure groundvaries mass 3f).The from ET-4 ET-5 ET-1 ET-3 ET-2 0 SCALE 5m Pseudonummoloculina heimi, Ovalve and Cuneolina - - - /2019 4.2.2. NEZZAZATINELLA PICARDI 4.2.1 PSEUDOLITUONELLAREICHELI In the interval studied we recognized two zones: theTethys Realm. partof inthewestern fers these benthic foramini distributiongeographic of the an important contribution to the knowledge of Mexico.ranean area and southern Moreover, itis peri-Mediter the from localities other in defined as mid–late Cenomanian,comparable with those this unit, which isdetermined accurate dating of consequently,study this provides asupportfor an theVSLPP; iferal studies frompart of the western Few datingshave benthic foramin beenbasedon dating thesedeposits. make these fossils tool fora useful biostratigraphic dance, diversity, andevolutionary rates, which value stratigraphic is based on their abunTheir possibly Turonian age; however Saint-Marc (1974) P. that reicheli indicated (1985) Neumann and Schroeder manian age. mid–late Ceno consideredrange and is tobeof material is mostimportant foraminiferThe in the studied disappeared wasdrowned. when theplatform mocalculus gymnocodaceans,such as A proliferation of binella mesogeensis, Praechrysalidina of community to forms Merlingina onella, Pseudocyclammina, Hemicyclammina, Daxia blage in which thelarger foraminifera by a change in the benthic foraminiferal assem reicheli Interval Zone, which overlies the cenomana, Pseudocyclammina Spiroloculina picardi, Nezzazatinella inflata, Minouxia N. Peneroplis simplex, parvus, Dicyclina schlumbergeri, Nezzazata gyra, Cuneolina parva, Cuneolina pavonia, clammina sigali, Daxia cenomana, Merlingina cretacea, blage of composed Assemblage Zone containsaforaminiferal assem overlain Pseudolituonella reicheli Assemblage Zone which, ischaracterized i pce anyo Cenomanian and a speciesmainly of is Nezzazatinella picardi , isobserved. association This later also disappear, reducing theforaminiferal Pseudolituonella reicheli Pseudolituonella reicheli, Hemicy Assemblage Zone andthe Nezzazatinella picardi, Rotor sp., and Interval Zone. , which hasashort sp., andmiliolids. Charentia Pseudolituonella Pseudolitu sp. , and Per ------marker. Recently, Frijia used thismicrofossilas alate Cenomanian zonal west central Jordan. In Turkey, Sari that the Cenomanian.Schulze (1964), andSampó(1969)recordedin thisspecies (Reiss,nian BozorgniaIran, Banafti In and 1957). it is recorded in the late Cenomanian andTuro P. reicheli Croatia and Decrouez (1977) in Greece reported theCenomanian. Husinec ical of Saint-Marc, 1966). Bilotte (1984) considered this speciestyp 1965; 1962, (Neumann Aquitaine P. reicheli author used limited ifer is to the upper Cenomanianrocks; this occhini the Cenomanian ( of Crescenti (1962)alsofound the species at the top a late Cenomanian age to Italy,Lebanon. In Luperto-Sinni(1966) assigned fromspanning to Turonian themid–Albian in assigned the taxon range alongstratigraphic Maritime region. InSpain,Barroso(2004) found Charente the in (1996) Moreau and (1965) mann considered a mid–Cenomanian speciesby Neu to berestricted appears to theCenomanian.Itis AudignonFrance;in theyindicated thatgenus this described by Cuvillier and Szakall (1949) from a mid–late Cenomanian age. specieswas This examined is Another importantfoundspecies the materialin late Cenomanian. Michaud (1987) regarded this speciesasmiddle– dle-upper Cenomanian. Inthe Chiapas region, the Guerrero–Morelosin upper mid in Platform lituonella reicheli In Mexico, Aguilera-Franco (2003) situated and pithonellids( opportunist planktic foraminifers of with deposits time this in platform the of flooding complete the zone); however, inthe studied material we recorded latest Cenomanian ( be correlated bycarbon isotopestratigraphy to cated that at this speciesdisappears levels that can P. reicheli from the mid–late Cenomanian. InIsrael, et al is reported is from the Cenomanian inW . (1979,1984)stated that this foramin P. reicheli only occurs inthe Cenomanian in onlyoccurs Daxia cenomana inthe Whiteinella archaeocretaceaWhiteinella asazonal marker. InFrance, Cisalaveolina fraasiCisalaveolina Neocardioceras juddi Pseudorhapydionina dubia Pseudorhapydionina et al. P. reicheli et al. (2015, p. 129) indi 129) p. (2015, , which determines , which determines (2004) indicated etal. ; Sartoni and Zone).Chi et al. ammonite Zone). (2000) in (2009) Pseudo Zone Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín ------it as mid–Cenomanian. Gräfe (2005) recorded (2005) Gräfe mid–Cenomanian. as it Daxia cenomana f h eoainadtebs fthe Turonian. the Cenomanian andthe base of of regardedrestricted thespeciesas to themiddlepart the Cenomanian. Schroeder and Neumann (1985) Israel byHamaoui andSaint-Marc (1970)asfrom Cenomanian age.described from Itwas Negev, is samples examined the in identified form Another Cenomanian inEgypt. document the occurrence of age in the Iberian Range. Ismail regarded this speciesasearly–mid Cenomanian the Basque–Cantabrian Basin. Caus cenomana at f te SP (oe, 96 Tavitas 1956; (Bonet, VSLPP the of east and Cenomanian strata; it has been reported from Mexico,In ated withthemid–late Cenomanian species. clina schlumbergeri inthe studied samples is An abundant form marker from theSergipe BasininBrazil. considered (Mouty Cenomanian. It has alsobeen recorded in Syria documented the presence of (2009) Shirazi Turkey. area, Dağ this speciesinthe Cenomanian inthe Katran, Tethyan areas. Bignot and Poisson(1974) recorded a particularlyuseful Cenomanianmarker many in in the Lusitanian Basin, they stated that the Rio Mondego to outcrops along the valley of Hart Portuguese the western in manian Later,Basin. the occurrence of dle Cenomanian age. Berthou (1984a) recorded mid the to it assigned He (1953). Maync by time Hemicyclammina sigali is associated with mid–late Cenomanian, takingintoaccountthat it is inthe studied samples Other form conspicuous Cenomanian rocks intheIberianPeninsula. Caus 1984) aswell as inthe Morelos Formation in the Merlingina cretacea Hemicyclammina sigali, et al. et al. et al. inthe Cenomanian andTuronian from (2009)foundspecies inmid–upper this 20) tde a abnt succession carbonate a studied (2005) D. schlumbergeri H. sigali , 2003). Berthou and Bengtson (2007) from the Burgos Province, dating Munier-Chalmas (1887), associ H. sigali Pseudolituonella reicheli. H. sigali , which confirms the mid–late the confirms which , to be a reliable Cenomanian was described for the first first the for described was which isalsoconsidered is very is Albian in common in Iran in the mid–lateIran in in restricted to theCeno D. cenomana /2019 et al. et al. H. sigali from the (2009) (2009) et al Dicy 701 701 D. D. is ., - - - -

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 702 702 (Ponce 1984). deLeón,1983;Ornelas, Tepalcatepec Formation in Jalisco andColima in the Veracruz Basin (Sohl species hasbeen found inthe Orizaba Formation in the Chiapas Range (Michaud, 1987).This Allison, 2005), and in the Sierra Madre Formation Guerrero–Morelos (Aguilera-Franco Platform and recognized inourmaterial. ronmentssupply, and the terrigenous been ashas shallow marine envi interval byeutrophication of occurred in the Cenomanian/Turonian boundary all the benthic foraminifera extinctionThe of Castro, 1965;Schroeder andNeumann,1985). cies isconsidered as mid–Cenomanian age (De that given in other publications, in which the spe distributionstratigraphic could be extended from eroplis parvus We assigned a mid–late Cenomanian age to Cenomanian (Velić andVlahović, 1994). Croatia, age fromthe Varassova Greece.in Mountains In this speciesislate Albian to early Cenomanian (1980) mid–Cenomanian. According to Fleury to Albian latest the from ranges form this (1985), analyzed. According to Schroeder and Neumann Peneroplis parvus strata (Arnaud-Vanneau and Premoli-Silva, 1995). knownis from Albian toCenomanianin Tethys ples is A commonspeciesfound inthe analyzed sam middle–upper Cenomanianstrata. (Sari Husinec Slovenia byKoch Italy (Luperto-Sinni 1966andSpalluto, 2012),in in recorded been also has It 1958). Conkin, and in Texas, andLouisianainUSA(Conkin Florida, of distribution and stratigraphical to thatgraphical age.Mexico, In a similargeo thisspecieshas inthe Canyon VSLPP. ElAbra He assigned it an Albian/Cenomanian the from time for first (1956) the Bonet by described was species The heimi usualoccurrenceof The / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Dicyclina schlumbergeri wasrecorded in the material examined. et al., Cuneolina pavonia etal. P. parvus 2009)andSyria(Ghanem in the material in its studiedandthus (2000); it is alsoregistered in Turkey is a common speciesinthe samples was determined tobeinthe late determined was et al. (1998),andinCroatia by . The species is recorded speciesis . The d’Orbigny.species This et al Pseudonummoloculina ., 1991) and the et al ., 2012)in Pen - - - - - /2019 4.3. PALEOECOLOGY ANDPALEOENVIRONMENT El AbraLimestone. tant the because age it constrains assigned tothe Cenomanian/earliest Turonian, which isimpor Range Zone, which hasbeen regarded as latest recognized as the nella, Gavellinella benthic foraminifera; for example, baltica, W. paradubia,W praehelvetica, archaeocretacea,Whiteinella W. W. aprica, brittonensis, W. rioensis, M.planispira, Heterohelix moremani, H.reussi, strategist planktic foraminifers Formation witha bonates are overlain by the hemipelagic Soyatal El Abra Cenomanian shallow-waterThe car Glenn, 1986; Murray, 2006). nate under lower conditions(Hallockand energy predomi dwellers sediment and algal-film while andperiphytonencrusters are the most common, environments,faunal, infaunal). In higher energy the sediment(epi or in on or living eous algae), ers, periphytonand calcar (free-living on seagrass Recent larger foraminifera may occurasencrust supported is by assemblageThis study. the modern 1965). (Haynes, environments low-light quiet in maximum surface-to-volume ratios will be found environments while thinfragile tests with reef with robust sphericaltests indicate current-swept Thus,mental interpretation. detached life forms factor provides animportant tool for paleoenviron the foraminiferal test as well the hydrodynamicas of shape the on symbionts the of influence The main factorrequiredbecause itis bythe symbionts. distributiondepth isrelated to light, which isthe waters(Murray, warm 1991).Their indicative of largerThe symbiotic-bearing foraminifera are er-Fadel, 2008). Cenozoic (Hohenegger, 2000, 2004;BouDagh had a similar distribution in the Mesozoic and and hydrodynamicenergy. inferred It is that they ture, light intensity, nutrient content, substrate, distribution are controlled patterns by tempera environments,In modern benthicforaminiferal andtextularids.interval This is Pithonella Whiteinella archaeocretaceaWhiteinella acmeandthe Muricohedbergella del Muricohedbergella and other small Lingulogavelli r and Partial r-k ------

such asrudists, gastropods, and echinoderms, foraminifers, and invertebrates together with algae the benthic great varietyThe and diversity of aggregatum Neomeris cretacea parvus. N. Nezzazatinellagyra, simplex, picardi Pseudocyclammina sp., Dicyclina schlumbergeri, Nezzazata parva, cretacea, Cuneolina pavonia Cuneolina pavonia, Hemicyclammina sigali, Daxia cenomana, Merlingina foraminiferal assemblage, composed of benthic diversified and abundant and ElTemazcal sections,characterized is byan Cerritos studied successions, Llanosdel Carmen, El Abra FormationThe (Taninul Facies) in the existed duringtheElAbradeposit. struct the paleoenvironmental thatconditions as lithologic characteristics were used to recon other biogenic componentssuch asalgae, aswell study,In this benthicforaminifera, together with (Hallock andGlenn,1986). phytic (Langer, forms 1993) or living insea grass Recent indicating a decrease of benthic-factory carbonate benthic-factory indicating adecrease of disappear, reducing the assemblage to small forms, adapted to oligotrophicaminifers to conditions that caused the largerto the platform sized for associated with changes inthe nutrient supply benthic foraminifera indicates a marine deposit of as well algae as decreased diversity abundance of the algae Nezzazatinella picardi, is reduced to a few benthic foraminifers such as El AbraFormation. foraminiferal The community the changeTherea conspicuous is the topof in indicate mediumhydrodynamic energy. parvovesiculifera Thaumatoporella Dicyclina, Cuneolina, coidal andconicalbenthicforaminifers such as dis large-sized of occurrence The flourish. and this oligotrophic association to developpermitting during stable salinity andtemperature conditions, the euphotic zone on the open marine platform rock, a shallow-watersuggest environment within the texturebioclastic packstone–grainstone of tubes, calcareouswell as worm the peloidal as The algae recorded algae The are Peneroplis and Permocalculus irenae Permocalculus , aswell as the encrusters Thaumatoporella parvovesiculifera Thaumatoporella and adteecutn ai f andtheencrustinghabitof miliolids, androtalids, and Spiroloculina and Pseudolituonella reicheli, Bouenia pyigmaea Bouenia pyigmaea and are knownas epi P. budaensis. , and Lithocodium, Lithocodium Peneroplis . The The and Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín - - - - 4.4. SYSTEMATIC PALEONTOLOGY vrbnac fpithonellids, overabundance of a foraminiferal with an packstone–wackestone overlies the El Abralimestone, whichof consists Soyatal The theplatform. Formation drowningof production (Schlager, 1981),which preceded the La Minitaoutcrop, which ischaracterized by a the El Abra facies, isrecordedtion, termed in the the El AbraForma faciesof A lateral change of Partial RangeZone). in thelatest ( Cenomanian the transgression phase that of flooded the VSLPP and lithological changes are related to an early faunal significant These environment. eutrophic as gavellinelids, which indicate and a deeper such foraminifers benthic different and planktic, dad NacionalAutónoma deMéxico). (Universi Geology the Institute of Collection of thin sectionsareThe housed inthe Paleontology (2013 partim). foraminifera,the agglutinated and Pawlowski classification proposedthe (2014) for Kaminski by foraminiferalagglutinated based on assignment is dant and well preserved. newsuprageneric The the El AbraFormation are abun stone samplesof benthicforaminifers contained in the lime The shallow-water environment. semi-restricted allow usto infer an intermediate olinids, loculina heimi speciesincluding a larger diversity of showing identified is microfacies Other ronment. characteristics a restricted suggest shallow envi within environmentssalinities,with varying these abundant miliolidsandostreids adapted to survive cream limestonerepresented bya wackestonewith Superfamily Nezzazatoidea HamaouiandSaint- Subclass GlobothalameaPawlowski Holzmann Class FORAMINIFERAd’Orbigny, 1826 Suborder Nezzazatina 2004 Kaminski, Dicyclina schlumbergeri Order Lituolida Lankester, 1885 and and Tyszka, 2013 Ovalveolina maccagnoae Ovalveolina Marc, 1970 Whiteinella archaeocretaceaWhiteinella and r and Cuneolina pavonia /2019 Pseudonummo , other alve r-k strategist et al 703 703 ------.

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 704 704 Charentia Figure 8 sp. subaxial(SampleLLC-2). section whorls, showing arounded proloculus, the cham Description: and Tappan, 1988,p. 71,pl.55,figs. 1–4. and Saint-Marc, 1970,p. 304,pl.18–21;Loeblich Biconcava bentori / Type species. Family NautiloculinidaeLoeblich andTappan, Mid–lateCenomanian foraminifera from theElAbraFormation (scalebar200µm).a: Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín sp. equatorial section(SampleG-2)LLC-1); c: Genus Biconcava bentori Test planispirally coiled with three aau 16, . 4 Hamaoui 14; p. 1965, Hamaoui Biconcava

Biconcava bentori (Figure 8a) 1985 Hamaoui,1965 Hamaoui Hamaoui,1965 , 1965 Daxia cenomana - /2019 groove intheapertural face.” evolute and inthe aperture located in avertical in appearance to stated, authors genus“this isclosest former The byHamaoui andSaint-Marc (1970,p. 301). tooth plate described internal a rudimentary of ferred Remarks: curved lastwhorl in.The has 18 chambers. growing bers slowly;curved sutures, but slightly equatorial section (SampleLLC-1); equatorial d: section Type species: G enus Biconcava Loeblich andTappan (1988) trans Daxia toMaycinidae due the absence Biconcava bentoriBiconcava Cuvillier andSzakall,1949 Daxia Szakall, 1949 Daxia cenomana but differs in being more being in differs but tangential section; b: tangential section; Cuvillierand Pseudocyclammina -

roso, 2004;Caus Spain (Calonge and Caus, 1996; Gräfe, 2005; Bar and Szakall, 1949; Neumann, 1965; Bilotte, 1984), Francein recorded(Cuvillier been has and 1985), ical Tethysianspecies (Schroeder and Neumann, Occurrence: torial section. and suturesthinner septa lessdepressed inequa its largerin size,(Pyrénées Basco-Béarnaises), minima Remarks: theproloculus is30mµ. the diameterof µm; 700 to 500 from varies height measured The material 12–16chamberspossess inthe last whorl. gated with curved sutures.in our Some specimens chambers; the latest chambersare low andelon rounded proloculus followed by rhomboid-shaped Description: 1–8.1. figs. 1, pl. 15, p. 1985, Neumann, and Schroeder fig. 3; 11, pl. 55, p. 1952, Maync, 4–6; figs. 2, pl. Daxia cenomana uncoiled and finally flaring; broad and low cham low and broad flaring; finally and uncoiled angular section withinitialpart planispiral, later Description: 1987, pl.12,figs. 1–12. Michaud, 1–9; figs. 15, pl. 37, p. 1–8, figs. 1, pl. 1985, Neumann, and Schroeder 22–27; pl. 315, pl. 14, fig. 14; Hamaoui and Saint- Marc, 1970, p. Merlingina cretacea Cerritos, andTemazcal sections. VSLPP, it was recorded in the Llanos del Carmen, (Ismail 1984b; Berthou andLauverjat, 1979), andEgypt Type species: Family Nezzazatidae HamaouiandSaint-Marc, Subfamily Nezzazatinae HamaouiandSaint- Daxia cenomana Laug and Peybernès (1979) of the Aptian the Aptian Laug and Peybernès (1979) of et al. Merlingina cretacea Genus , 2009;Anan Daxia cenomana The specimen illustrated specimen The a tri is Cuvillier and Szakall, 1949, p. 8, Daxia cenomana Merlingina Test planispirally coiled; with a

Merlingina cretacea Hamaoui, 1965, p. 7, pl. 9, fig. 6; (Figure 8c,9a) et al CuvillierandSzakall,1949 Marc, 1970 (Figure 9c) ., 2009),Portugal (Berthou, 1970 Hamaoui,1965 Hamaoui,1965 et al., differs from differs isconsidered a typ 2013). Hamaoui,1965 Daxia Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín ------Italy (Chiochini and Saint-Marc, 1970). It hasbeen recorded in samplefroma subsurface Negev, Israel(Hamaoui Occurrence: Marc, 1970). a more complex tooth plate (Hamaoui andSaint- sutures more complex aswell as the aperture with spire, and specimens, with rapid enlarging of Biconcava Remarks: sutures sinuous. thepreceding chamber; of ing totheseptum face, having two orthree basal digitations attach the apertural inward from the lateral borders of bers,by subdivided tooth plate slightly curved blich andTappan, 1988,p. 83). orifice, flattened a with tooth-likeoutgrowth (Loe anL-shaped the bend nearlyperiphery; forms face bending below wall parallel to the the dorsal the apertural the umbilicalregion at thebaseof area aperture closed. The extending from near backwards away from the apertural face, umbilical small indentation suture, inthe septal which points ventral sutures radial, slightly depressed witha the chambersincreasing slightlyinsize asadded; tral side convex, area dorsal moderately convex; Description 286, figs8 b, c. 2004, p. Andreu, and Ettachfini 1–11; figs. 11, pl. p.33, 1985, Neumann, and Schroeder 13; fig. 40 7–13; Hamaoui and Saint-Marc, 1970,p. 348,pl. Nezzazata simplex section. VSLPP intheLlanosdelCarmen 1993). 2003), and inPeru (Jaillard andArnaud-Vanneau, the Morelos Guerrero (Aguilera-Franco, Platform from(Michaud, 1987)and Mexico Platform the Chiapas in identified was species this Americas, al. 2009), Turkey(Sari Type species: , 1995), and Syria (Ghanem Syria and 1995), , by having anuncoiledstage in adult Genus Nezzazata simplex

Merlingina : Test sub-circular, trochospiral, ven

Merlingina cretacea Fgr fand9g) (Figure 9f Omara, 1956, p. 887, pl. 102, figs. Nezzazata

et al. Nezzazata simplex et al. differs from differs , 1984), Spain (Caus , 2009),Oman(Philip Omara,1956 Omara,1956 et al., was described from was /2019 Omara,1956 Nezzazata 2012). In the et al. 705 705 and et - - - ,

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 706 706 (Sample LLC-1). e: (Sample ET-4); c: Daxia cenomana Figure 9 Hemicyclammina sigali / Mid–late Cenomanian Mid–late foraminifera from theElAbraFormation(Allscalebarsf, 200µmexcept gscalebar 500µm.a: Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín equatorial section (SampleET-4); equatorial b: section Merlingina cretacea equatorial section equatorial(Sample LLC-1); section f, g: oblique section (SampleLLC-5); d: obliquesection Nezzazatinella picardi /2019 Nezzazata simplex Nezzazata gyra equatorial section onthespiraland equatorial section theumbilical side equatorial section equatorialon spiral section and umbilical side obliquesubequatorial (SampleET-4); section apas Platform (Michaud, 1987) and the Guerreroapas Platform Mexico,2012). In been found ithas the Chi in and Turkey(Sari (Simone been recordedhas fromItaly the Cenomanianin recorded it in the late species Cenomanian. This stratigraphic range to the early the Turonian. Ismail extended (1965) Strauch and zazat, west central Sinai by Omara (1956). Omara Gebel Nez the Cenomanian of the lower part of Occurrence: and Sliter, 1995). it doesnothave the tooth plate (Arnaud-Vanneau could be incorrectly assigned to Omara and Strauch (1965) is poorly described and cave spiral view. Hauterivian cava convexdistinct from planispiral side; andis to slightlyconvex spiralsiderather than astrongly from ical side anda smaller umbilicus. from Remarks: aperture. veloped tooth plate which extends to the previous well-de a and size larger having by 1995) Sliter, early Albian and froma falseumbilicus possesing the Aptian– Remarks: with anaperturaltooth. or indentation suture, inthe septal typicalaperture tothe previous resultingseptum a kink septum in platea narrow extendingfrom back internal one on the spiral side; umbilicus closed, chambers with Description: 1985, p. 34,pl.12, fig. 9. Nezzazata gyra Beggia zar sections. andGuadalca VSLPP in the Llano del Carmen found inHondurasby ScottandFinch (1999). (Aguilera-Franco,Platform 2003). It has alsobeen (Smout, 1956) because it has a strongly con strongly a has it because 1956) (Smout, N. simplex N. convexa gr. gr. et al. gyra Nezzazata gyra

Nezzazata gyra Nezzazata conica , 2012), Croatia (Husinec Smout, 1956, p. 340, pl. 1, figs. 1–9; (Smout) Schroeder and Neumann, Test plano-convex withthree whorls

N. isabellae bya verypossessing convex umbil (Smout, 1956) by possessing a flat a possessing by 1956) (Smout, Nezzazata et al (Figure 9d) ., 2009);Syria(Ghanem (Smout,1956)

(Arnaud-Vanneau and differs from simplex (Smout, 1956) differs differs 1956) (Smout, Nezzazata germanica wasrecorded in Nezzazata N. simplex N. simplex et al. et al. because , 2000), (2009) N. con differs differs et al., Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín by by ------

and Cerritos sections.and Cerritos Guadalcazar VSLPP in the Llano del Carmen, 2006), andTurkey (Farinacci andYeniay, 1986). and Masse, Iraq(Bernaus 2009), thesubsurfaceof Syria (Ghanem Croatia1966), southern (Husinec from the Cenomanian inItaly (Luperto-Sinni, Occurrence: and strongly curved sutures intheumbilicalview. morewith alobate than1mm, margin, and angled a test in later species that measures side inplace of less elongated, and radial sutures inthe umbilical ing asmaller test, a rounded periphery, chambers mian/Aptian Nezzazatinella picardi in theumbilicalside. inthe last whorl,bers and more depressed sutures cham more having by Kenawy,1957) and (Said Turonian from differs species This curved row or scattered over the apertural face. and a chambers larger apertureapertures with secondary ina shaped differently and fewer Coniacian Remarks: and Tappan, 1988). regionthe umbilicus 1948a; Loeblich (Henson, aperturesondary inacurved row orscattered over area is wide with a large curved slit, may have sec last whorl, sutures radial, depressed; theapertural inthe 11 chambers backwards, flaring chamber whorls; they are narrow, elongated, with the last slightly convex; in 1–2 withchambers arranged Description: pour-Bonab i; Sari (Henson) Aguilera-Franco figs.3–6; 18, pl. 1,3, figs. 15, Valvulammina picardi Type species: et al. Nezzazatinella picardi Genus N. adhami , 2009, p.2009, , figs.2, pl. 60, Rahim 13; 12,

Nezzazatinella picardi et al. N. macoveii Test trochospiral, side dorsal flat or Nezzatinella Nezzazata gyra

et al. , 2012,p. 28,fig. 8 p. Nezzazatinella adhami 1976, p. 492 Henson, 1948a,p. Henson, 613,pl. (Figure 9b) isdistinguishedfrom Barre Darmoian (1976) by having Darmoian , 2012), Egypt (Ismail , 2012),Egypt Neagu (1979) byposses Darmoian, 1976 Darmoian, et al. (Henson, 1948a) has been reported has Nezzazatinella picardi , 2001, p. 248, fig. 9 differs from pre– from differs /2019 N. aegyptiaca N. aegyptiaca et al. Darmoian, Darmoian, , 2009), et al 707 707 ., - - - - -

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 708 708 non, Iran, Slovenia, Croatia, Turkey, andPortugal Israel, Leba from the Albian andCenomanian of comparable to it were later described and drawn (Henson,1948a). Forms Egypt Santonian beds of as time first the for Cretaceous rocks.described was species This Occurrence: tion). Inaxial section that are almostquadrangular (in equatorial sec chambers at to form the test periphery right angles latter in contact with the septa species possesses Albian Remarks: (Maync,septa 1953; Loeblich and Tappan, 1988). semi appearing very shortandoriginally termed the previousagainst whorl, inequatorial section coalesces asanimperforatethe septa basal layer layer alveolar; the lowerdermal uniformly part of outer layeragglutinated, imperforate, andsub-epi continuousstraight orslightly curved wall septum; a last chamber incompletely subdivided by a dis to subacute periphery, witha small proloculus, and Description: 5; 4, Shirazi figs. 3, pl. 232, p. 1970, Saint-Marc, 1–5; Hemicyclammina sigali Temazcal sections. Cerritos, and VSLPP the LlanosdelCarmen, in 1979). et al. Saint-Marc, 1970; Moro and Jelaska, 1994; Koch and Šribar, 1998;Hamaoui,1966;Hamaouiand (Reiss, 1961;Bozorgnia andBanafti,1964;Dozet Type species: / Suborder andMikhalevich, LoftusiinaKaminski Order andMikhalevich, LoftusiidaKaminski in Subfamily Hemicyclammininae Banner, 1966 Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín , 1998;Sari Family Cyclamminidae Marie, 1941 Genus et al. Hemicyclammina sigali H. whitei

, 2011,p. 783,pl.2,fig. 11. Hemicyclammina sigali Hemicyclammina Test planispiral, shows a rounded N. picardi

in Kaminski, 2004 in Kaminski, et al Hemicyclammina sigali Kaminski, 2004 Kaminski, (Henson,1948b) because the ., 2009,Berthou and Lauvejat, (Figure 9e) an, 93 p 18 figs. 148, p. 1953, Maync, Valvulammina picardi H. sigali occurs widely in Upper widely in occurs Maync, 1953 Maync, 1953 is more is compressed. differs from differs Maync, 1953 from the - - - - - /2019 VSLPP in the Llanos del Carmen VSLPP intheLlanosdelCarmen Brazil (BerthouandBengtson,2007). 2003), Jordan (Weidich andAl-Harithi, 1990), and 1974), Iran(Shirazi, 2009), Syria (Mouty (Simone is recorded in Portugal by Hart the Constantine Province species inAlgeria. This by Maync (1953) from the middle Cenomanian of Occurrence: producing test. apeneropliform and large test with chambersincreasing inheight, by having wall agglutinated a thick andcoarsely masi Coniacian/Santonian The bers and apertural surface solid,noncanaliculate;bers theearlycham pseudoalveolar structure; wallof by cylindricalcanaliculi resembling keriotheka or rounded;is periphery imperforate wall pierced uncoiled with ten chambers inlast whorl; the Description: Cerritos, ElTemazcal sections. Occcurrence: pan, 1988). (Loeblich wall and septa agglutinated andTap with numerous alveoles closely spacedinthe network with athick subepidermical agglutinated growing rapidly; sutures oblique, wall coarsely three whorled chambers composed of periphery; Description: Type species: Genus Type species: Family Charentididae Loeblich andTappan, (Schlumberger, 1899) differs from differs 1899) (Schlumberger, Subfamily Choffatellinae Maync, 1958 Superfamily Biokovinacea Gŭsić,1977 Suborder Biokovinina 2004 Kaminski, Pseudocyclammina Genus et al. , 2012),Turkey(Bignot and Poisson, Test planispiral later partly Test planispiral with arounded

Hemicyclammina sigali Pseudocyclammina VSLPP in the Llanos del Carmen, VSLPP in theLlanosdel Carmen,

Charentia Cyclammina lituus Charentia cuvillieri Charentia (Figure 8b) (Figure 8d) 1985 Yabe andHanzawa, 1926 Neumann,1965 sp. Hemicyclammina chal sp. Yokohama, 1890 et al Neumann, 1965 was described was . (2005), Italy (2005), . H. sigali et al. - - - , liform, early trochospireliform, followed by very broad, Description: p. 423,pl.3–7. 1; Tasli figs. 50–52; Chiocchini Cuneolina pavonia Occurrence: chambers. lieri Remarks: chomata-like projection. a triangular aperture distinctly thickened to form the apertural surface beneath the the portion of and Sliter (1995) by having a larger size and flabel Aptian/Albian havinga broader test. Santonian Cuneolina pavonia neau andPremoli-Silva, 1995). Arnaud-VanSliter,1995; (Arnaud-Vanneauand than be slightlylarger and have agreater apical angle Henson. are Remarks: Tappan, 1988,p. 48). layerreticulate (cf. subepidermal Loeblich and imperforate, wall agglutinated, ing the septa; with biseriality, andbyof horizontal partitions parallel outer wall and projecting inward toward the plane to the radial partitions positioned perpendicular into nearlysubdivided rectangular chamberlets by biseriality; interior pressed parallel to the plane of low chambers, biserially arranged com commonly Type species: Superfamily Ataxophragmiacea Schwager, 1877 Suborder Ataxophragmioidea Schwager, 1877 Neumann (1965) by having fewer whorls and whorls fewer having by (1965) Neumann Cuneolina pavonia Subfamily CuneolininaeSaidova, 1981 C. parva Family CuneolinidaeSaidova, 1981 et al. Cuneolina pavonia Genus C. pavonia

The two The speciesreported most often Cuneolina conica Charenti , 2006, p. 529, fig. 6 L; Sari Test compressed conical to flabel to conical compressedTest (Figure 10aand10b) , whichconical andelongateis VSLPP the El Temazcalin section. Cuneolina

d’Orbigny, 1846, p. 253, pl. 21, pl. 253, p. d’Orbigny,1846, Cuneolina sliteri Cuneolina pavonia d’Orbigny (1846) differs from differs (1846) d’Orbigny a sp. differs from is flabelliform and tends to tends and flabelliform is d’Orbigny and et al d’Orbigny, 1839 d’Orbigny, 1846 C. pavonia ’rin (80 by (1850) d’Orbigny ., 1984 p. 181, pl. 5, fig. Arnaud-Vanneau d’Orbigny, 1846 differs from differs Charentia cuvil et al C. parva C. parva ., 2009, Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín ------conch covered by a deuteroconch followed by a alarge, oval proto apparatusonic of composed Description: 184, figs. 4,11–12. p. 2011, Scott, and Filkorn 6–9; figs. 4, pl. 1995, Cuneolina parva Arnaud-Vanneau and Sliter, pl.14, figs. 1–6, pl. 17, figs. 7–12, pl. 18 figs. 12–14; parva Cuneolina pavonia Cerritos, Temazcal sections. Occurrence: biserial stage with 6 or 7 chambers inlater species. atriangular test with ashort test instead of liform Remarks: rectangular network.that produce a subepidermal byradial beams, andoneortwo transverse rafters biseriality and subdivided parallel to the plane of broad, low biserial stage. compressed Chambers Premoli-Silva, 1995), and in Mexico: as Mexico: in and 1995), Premoli-Silva, gin inFrance and Spain (Arnaud-Vanneau and mar and NorthAfrica,fromthe northern Greece,East, Egypt, Italy, Albania, Yugoslavia, the Tethysin the Middle margin of the southern Occurrence: lar testandalmostcylindricalearly stage. latter(1948a). The a remarkablepossesses triangu to the Maastrichtian Iraquian tranverse rafters. of network dense radial partitions andmore common occurrence of a having by (1958) Dalbiez C. parva andScott,2011). Albian toSantonian(Filkorn Cenomanian strata and 1995). Premoli-Silva, Arnaud-Vanneauand Sliter,1995; to onetwo in three transversein the chambers compared rafters than a smaller apical angle sphere andsmaller biserial stage as well as having bya smaller possessing test with a large megalo from differs species This Egypt. (1948a) son from the Santonian of Cuneolina parva differs from Barremian/Aptian Barremian/Aptian from differs Cuneolina parva

Cuneolina parva Test compressed, conical.Embry VSLPP in the Llanos del Carmen, VSLPP in the Llanos del Carmen, The speciesismostlyknown from The (Figure 10cto10f) C. parva C. parva C. pavonia Henson, 1948a, p. Henson, 624–627, is reported is fromAlbian– C. pavonia Henson,1948a issimilarincrosssection (Arnaud-Vanneau and was described by was Hen C. pavonia C. cylindrica d’Orbigny (1846) from uppermost from uppermost /2019 hastwo to C. hensoni Cuneolina Henson 709 709 ------

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 710 710 schlumbergeri showingequatorialproloculus section (SampleG-5); h: thegreat Cuneolina parva pavonia Figure 10 / axial section (Sample ET-1); c: axialsection Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Mid-lateCenomanian foraminifera from theElAbraFormation. a: axial section subequatorial (Sample LLC-2);axial section j: section axial section (SampleLLC-5); f: axialsection Cuneolina parva Cuneolina parva axial section (Sample LLC-5); axialsection d: /2019 axial section (SampleLLC-5); g: axialsection Dicyclina schlumbergeri Dicyclina schlumbergeri Cuneolina pavonia Cuneolina parva subaxial (SampleG-5). section axial section (SampleLLC-5);axial section i: axial section (SampleG-5);b: axialsection Dicyclina schlumbergeri axial section (SampleET-1); e: axial section axial section axialsection Cuneolina Dicyclina rior subdivided by numerousthin radial partitions, the test, inte oneither side of added alternating chambers annular Later µm. 700 measuring ulus theproloc alospheric generation solelyof consists meg the inflated; slightly stage undulating,initial Description: 5–7; Sari pls. p. 406, p. 1956, Bonet, fig. 2; 363, fig.p. 1, 362, 1904, Choffat, and Schlumberger xxx-xxxi; 1887 dalcazar, andtheElTemazcal sections. Cerritos, Gua del Carmen, VSLPP the Llanos in 1947). face samples(CushmanandApplin, from subsur and Scott, 2011); in Florida Filkorn walteri esi h pems ato the supraembryonic part of lets in the uppermost chamber thesecondary havinga speciallayer of from fers the Iranian Cenomanian complex embryon (Figure 10g). valid because the Mexican specimenshave a large, to mens apparatus.megalospheric We assignedour speci the embryonic development of ferent of degree dif the on based differentiated were taxa These and the Coniacian/Santonian least two species the mid–Cenomanian showed these authors that Albian to Maastrichtian (Bilotte, 1984);however, Dicyclina that Remarks: network (Loeblich andTappan, 1988). organizedbeams and rafters in a subepidermic exoskeleton The imperforate comprises epidermis. chamber tochamber. Wall with an agglutinated to the outer wall and aligned from perpendicular Family Dicyclinidae Loeblich andTappan, 1964 Dicyclina schlumbergeri Type species Dicyclina Genus (in Scott and González-León 1991, p. 58; p. 1991, González-León and Scott (in Dicyclina schlumbergeri

schlumbergeri D. schlumbergeri, et al. Cherchi andSchroeder (1990) stated Dicyclina was until recently was assignedsolelyto , 2009,p. 61,pl.3,figs. 8,9. Test discoidal, flattened, slightly flattened, discoidal, Test (Figures 10gto10j) Chalmas, 1887

Dicyclina schlumbergeri , a taxon ranging from the late Munier-Chalmas, 1887 MunierChalmas, 1887 which we considertobe Munier Chalmas, p. Dicyclin D. schlumbergeri D. schlumbergeri. D. sampoi a comprises ata comprises Munier D. simplex bynot dif Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín ------

dalcazar, andElTemazcal sections. Cerritos, Gua del Carmen, VSLPP the Llanos in al. (Afghah 1986; Tasli, 2006;Robertson, nia (Polavder, 2003),Turkey(Farinacci andYeniay, and Masriera, 2006), the Vardar region, Macedo 1979), Slovenia (Koch coni in the Tethys;it has been reported in Italy (Chec Occurrence: zone (Cherchi andSchroeder, 1990). subembryonic part of zone andthe lowermost stage in aneccentric position, andathinner wall. because the latter species hasthe initial trochospiral Aptian Remarks: theapertural face. of turecribate is with numerouspores inthe center wall microgranular, bers; imperforate. aper The apertures but not completely crossingthe cham the circular jecting upward from the margins of sutures; interior chamber with tubular pro pillars lowuniserial chambers divided by depressed with a short trochospiral stage, later with broad, (1988, p. 155): Test elongate, conical, early portion Description: 2009, p. 61,pl.3,fig. 10. era-Franco Aguil 7–11; figs. 166, pl. 155, p. 1988, Tappan, and Loeblich 2; fig. 11, pl. 1987, Michaud, 1–9; figs. pl.8, 27, p. 1985, Neumann, and Schroeder Chiochini fig.1; text-fig. 10, pl. 1966, 149, Luperto-Sinni, p. 2a–b; Pseudolituonella reicheli Type species: Superfamily CoskinolinoideaMoullade, 1965 , 2005;Lézin et al. Suborder 2004 OrbitolininaKaminski, Family Coskinolinidae Moullade, 1965 P. conica Genus Pseudolituonella reicheli et al., , 2008),Portugal (Berhou andLauverjat,

Pseudolituonella reicheli et al 04, n Mrco (Ettachfini Morocco and 2014), Follows Loeblich and Tappan

D. schlumbergeri Pseudolituonella Luperto-Sinni and Masse (1993) etal.

., 2001,p. 248, fig. 9d; Sari 9d; fig. 248, 2001,p. ., et al. Pseudolituonella reicheli (Figure 11a) , 2012). , 1984, p. 181, pl. 5, fig. 15; fig. 5, pl. 181, p. 1984, , ai 15, . 117–119, p. 1954, Marie et al ., 1998),Spain(Ullastre Marie, 1954 Marie, 1954 iswidelydistributed differs from lower et al. /2019 , 2013), Iran Marie, 1954 et al., 711 711 et ------

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 712 712 section (SampleLLC-1); b: section Figure 11 section (SampleLM-5); g: section cenomanianus / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Mid–lateCenomanian foraminifera from theElAbra Formation(allscale bars200µm).a: (Sample LLC-5); e: Spiroloculina cenomana Minouxia inflata Ovalveolina maccagnoae axial section (Sample G-1); c: (SampleG-1); axial section axial section (SampleC-3); h: axialsection equatorial section (SampleLM-5);f: equatorial section /2019 Peneroplis parvus Ovalveolina maccagnoae axial section (SampleET-1); d: section axial Pseudonummoloculina heimi subaxial section (SampleLM-5). subaxial section Pseudolituonellareicheli subequatorial Archaecyclus axial sections. andCerritos VSLPP in the Llanos del Carmen above. distributiongraphical hasalready been discussed Tethysianspecies. andstrati Itsgeographical Occurrence: portion. twoonly sessing orthree chambersin the uniserial uniserial stage compared to the latter species, pos reduced trochospiral stage, andmore developed P. mariae early stage. from different Barremian ilarneetisedo quadriserial cham instead of rial arrangement Minouxia and Zijlstra-Bessais(2002). central TunisiabyTronchetti Cenomanian bedsof Remarks: and Zijlstra-Bessais, 2002). region (Loeblich and Tappan, 1988; Tronchetti trematophore-like plate that covers the umbilical in circular openings inthe latest chamber on a consists that multiple aperture canaliculate, finely larger, sutures depressed; wall thin, agglutinated, chamber last the chambers, inflated and globular Description: figs. 1–4;pl.4,figs. 3–5 3, pl. 1–8; figs. 2, pl. 1–7; figs. 1; pl. p.541, 2002, inflata Minouxia Order Textulariida DelageandHérouard 1896, Minouxia inflata Subfamily MinouxinaeLoeblich andTappan, Type species: Superfamily Eggerelloidea Cushman,1937 Family Eggerellidae Cushman,1937 Gendrot (1968) byhaving a larger test and differs from Genre

Pseudolituonella gavonensis Pseudolituonella gavonensis P. reicheli emended Kaminski, 2004 emended Kaminski, ioxa inflata Minouxia Test conical, elongate, triserial with

P. reicheli Tronchetti and Zijlstra-Bessais, Pseudolituonella reicheli Tronchetti andZijlstra-Bessais,

Minouxia Minouxia guembelitrioides 1954, p. 119 (Figure 11b) differs from upper Santonian upper from differs Tetraminoxia 2002 1986 byhaving a streptospiral Marie, 1954 wasdescribed from byhaving a trise Foury (1968) is is a typical is Marie, Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín - - - - Cerritos, Guadalcazar, andTemazcal sections. Occurrence: sections likeSantonian inflata Minouxia wide inaconicaltest. chambers longer than ular chambers inplace of Gendrot (1963) by having alarger test and glob inflata Minouxia ing chambers. chambers, the last chamber covering the preced M. guembelitrioides inflata Minouxia throughout arranged bers as inthe latter genus. sections. Cerritos, Guadalcazar, andthe El Temazcal Occurrence: andatruncateber arrangement periphery. tacea Remarks: chini, 2008). calcareous, imperforate, porcelanaceous (Chioc is neck. Wall short a on commonly tooth bifid or simple of consists chamber final the of end open plane; aperture chambers added in a single at of one whorllength, in thelastpart with four pairs proloculus followed bya tubular chamber second and truncate sphaeric arrangement, periphery; coilingandshowing asigmoid changing plane of strongly carenate extremities; last chambers Description: II, fig. 1. Spiroloculina cenomana Subclass Tubothalamea Pawlowski, Holzmann, Type species: Order MiliolidaDelageandHérouard, 1896 due to the former having duetothe former a sigmoidalcham Superfamily MiliolaceaEhrenberg, 1839 Family Spiroloculinidae Wiesner, 1920 Spiroloculina cenomana Genus

Spiroloculina cenomana Test elliptical inoutline, with VSLPP in the Llanos del Carmen, VSLPP in the Llanos del Carmen, VSLPP in the Llanos del Carmen, VSLPP in the Llanos del Carmen, Spiroloculina showsglobular chambers inaxial differs from Santonian from differs is different from Maastrichtian from different is ai (94 b hvn fewer having by (1954) Marie

Spiroloculina depressa Tyszka, 2013 (Figure 11g) Chiocchini,2008, p. 187,pl. 1826 M. lobata d’Orbigny, 1826 Chiocchini, 2008 Gendrot (1963). differs from S /2019 d’Orbigny, M. conica . cre 713 713 - - - - -

Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION 714 714 VSLPP, theLaMinitalocality. localities from area. theMediterranean Coastandother the Gulf Albian/Cenomanian of Occurrence: coiling which changes irregularly. having more chambers per whorl and a plane of Campanian inflated test and a very thick wall.The Santonian/ ulina robusta and Chiocchini,2006). Senonian stage but a more developed final stage (Mancinelli havingtest a discoidal and amore reduced early from earlyto middleAlbianovoidal WSerbia. nian of Santonian-Campa the from 1977) Radoičić, and Italy; and the Senonian of Mexico; of manian P. heimi the Pyrenees, France; the earlyto middleAlbianof resented by four species: Remarks: wall calcareous porcelanaceous. stages, withmore than two chambers per whorl; bottle-neck (goulot) and at least in adult growth lute, withamegalosphere provided withamiliolid Description: figs. 6,7 Sari 5L; pl. 61, p. 1991, moloculina heimi 15; fig. 3, pl. 268, p. 1987, Michaud, Conkin and Conkin, 1958, p. 156, pl. 1, figs. 1–10; Nummoloculina heimi / Type species: Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Type species: Superfamily Alveolinacea Ehrenberg, 1839 Pseudonummoloculina heimi Family Alveolinidae Ehrenberg, 1839 Bnt 15) rm h Aba t Ceno to Albian the from 1956) (Bonet, Family Pseudonummoloculina The genusThe differs from differs Ovalveolina P. irregularis Test discoidal,streptospirally invo

(Bonet) Scott and González-León, Hauerenidae P. heimi

Alveolina ovum Alveolina Calvez, 1988 Bonet, 1956, p. 402, pl. 3, 4; 3, pl. 402, p. 1956, Bonet, Pseudonummoloculina heimi Pseudonummoloculina aurigerica (Figure 11f) P. robusta is widelydistributed in the Reichel 1936 Pseudonummoloculina P. heimi differs from differs et al. Schwager, 1876 P. aurigerica Calvez, 1988 P. irregularis (Torre, 1966)from , 2009,p. 62,pl. 4, (Bonet, 1956) d’Orbigny, 1850 byan possessing Pseudonummoloc P. aurigerica Calvez from P. heimi Pseudonum (Decrouez is rep is differs differs by by by by ------/2019 poorly known from the New World but Remarks: appearance inthelastwhorl; wallporcelaneous. subaxial sectionthe chamberlets have apyriform the chamber; in the gated occupies a third part of later whorls, appearing rectangular, preseptal passage elon first the from elliptical elongated, ous; inequatorial section the chamberlets can be and numer short chambers the flexostyle; a by planispiral involute, spherical proloculus followed Description: and Neumann, 1985, p. 106–109, pl. 50, figs. 5–7. maccagnoae Ovalveolina early stage planispirally coiled, later with or Description: 39, figs. 1–17; Tasli pl. 86, p. 1985, Neumann, and Schroeder 14–15; Peneroplis parvus Occurrence: (1993, p. 603). Peru northern byJaillard andArnaud-Vanneau mensis Further alveolinids Manantlan RangeinColimaState, Mexico. the tro, 1966from of the Cenomanian deposits (2012) reported and Scott, 2002; Mancini 2006). Omaña Coast in the Albian–Cenomanian (Scott, Gulf of mexicana such as to berelated area theto speciesin Mediterranean endemic tothe Caribbean Province, but appears (Aurora Formation).consideredspecies is This described from the Mexican Cenomanianstrata lina mexicana Type species: were reported from the Cenomanianin Ovalveolina maccagnoae Ovalveolina Family Peneroplidae Schultze, 1854 S. peybernesi hasbeen also recorded in somelocalities Peneroplis parvus Peneroplis The mid–Cretaceous The alveolinids are Fourcade, Tardy and Vila (1974) was The test of megalospheric form is form megalospheric test of The Test with a rounded proloculus, VSLPPintheLaMinitaoutcrop. De Castro, 1965, p. 345–348, pl. 1, (Figures 11eto11h) Moll, 1798,p. 91 Ovalveolina maccagnoae Ovalveolina

(De Castro, 1983). Peneroplis planatus (Figure 11c) Sellialveolina deMontfort, 1808 et al. DeCastro, 1966;Schroeder DeCastro, 1965 , 2006, p.529, pl. 6, fig. O. DeCastro, 1966 sp. and Fichtel and Streptalveolina Streptalveolina De Cas S. Streptalveo cf. et al. drori - - - - - o te is tm b D Csr (96 fromthe (1966) DeCastro by time first the for Occurrence: septula. chambers subdividedby or pillars interseptal a simpleinterior, while the family Soritidae has haschambers with eroplidae because thisform and Tappan (1988)settled it inthefamilyPen Loeblich later (1985); Neumann and Schroeder Peneroplis Loeblich and Tappan(1988). classification of vipeneroplis this character radial species lacks striae on the outside surface. By icus from differs It chambers.numerous more planatus Remarks: tothesutures.perpendicular ribs fine with alternating grooves numerous with calcareous imperforate porcelaneous; the surface pen flaring test. Sutureseropliform slightlydepressed. Wall a is in resulting width, in increasing without uncoilingstage; the chambersquickly bers in the first whorls, later forming an annular an forming later whorls, first the in bers cham five coiled, planispirally Testconvexlarge, dalcazar, andTemazcal sections. Cerritos, Gua del Carmen, VSLPP the Llanos in (Ghanem andKuss, 2013). Syria and and 2006), (Tasli, Turkey (Velić 1994), Vlahović, Croatia 1996), Caus, and (Calonge (Italy); this specieshasbeen recorded from Spain mid–Cenomanian from the Campania region Type species: Subclass GlobothalameaPawlowski, Holzmann Superfamily Planorbulinacea Schwager, 1877 Order Rotaliina DelageandHérouard, 1896 Si ad eay 15) eas te latter the because Kenawy, 1957) and (Said Family CymbaloporidaeCushman,1927 but wasplaced in the family Soritidae by Archaecyclus Silvestri, , according to the foraminiferal generic

Archaecyclus Peneroplis parvus differs by having a smaller size and size asmaller having by differs

P. turonicus

Planorbulina cenomaniana Peneroplis parvus and Tyszka 2013 Archaecyclus (Figure 11d) 1882 Silvestri. 1908 couldbe assigned to is like theRecent is P 1908, p. 134 sp. was described was Seguenza, P. turon Lae Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín ------. 5. Conclusions Occurrence: Tappan, 1988). each chamber (Loeblich and the lateral margins of in the early stage; after with stolon-like openings at aperturemiddle position. The is interiomarginal calcareous, perforated, having adark thinlayer in the suturesarrangement; are oblique, the wall h eoiso teuprpr fthe El Abra the upper part of of deposits The section. Carmen VSLPP been observedonly has inthe Llanos del Jaillard andArnaud-Vanneau (1993)from Peru. medium-high hydrodynamic energy. ma The withopen circulationter carbonate platform and shallow-wa awarm Abra Formationof consisting the El late Cenomanian) in the Taninul facies of (mid– episode first a was there that consider We interpretation. enable a moreogy reliable paleoenvironmental benthic foraminiferal association and the lithol the data provided by the of integration The and climate perturbations. Partial Range Zone) due to the large scale flooding Soyatal tookplace( deposit Zone later also disappeared when the hemipelagic that survived. The ciation whichreducedwas to afewforaminifers tains arichand varied foraminiferalbenthic asso The Interval Zone. Assemblage Zone andthe the El Abra Formation: the Two zones are proposed for thefromsections age-equivalent associations. totheMediterranean foraminiferal assemblagesThe and algal are studied here asmid–late Cenomanian. Abra shallow-water deposits, dating the succession the El in value age-diagnostic significant a have benthic foraminifera species of The succession. which are described and illustrated for the studied larger benthic foraminifera, of composed mostly Formation preserved a rich and diverse association Pseudolituonella reicheli

Archaecyclus Nezzazatinella picardi Assemblage Zone con sp. hasbeen recorded by Whiteinella archaeocretaceaWhiteinella Pseudolituonella reicheli Nezzazatinella picardi /2019 Interval 715 715 - - - -

RESULTS AND DISCUSSION / Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation CONCLUSIONS CONCLUSIONS / ACKNOWLEDGMENTS / Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation REFERENCES 716 716 Acknowledgments could berelated to increasing nutrient availability textularids) associationin withalgae.change This ( viving is recorded, with a few foraminiferal species sur benthicforaminiferal species diversity decrease of blages coincides withthisenvironment. Later, a benthic foraminiferal assem ximum diversity of preparing numerous thinsections. editorial handling. We thankJoaquín for Aparicio Vegacisco Vera (UNAMMexico) forprecise his acknowledge gratefully Dr. authors The Fran de Barcelona) for theobservations onthetext. and Dr. Esmeralda Caus (Universidad Autonoma thatsuggestions much improved the manuscript, Universit) for valuable and careful comments and Tulsa(Babeş-BolyaiBucur I. Ioan University)and W. Scott (Precision Stratigraphy Associates and assistance. We are very to Drs.grateful Robert field logistical providing for Potosí) Luis San de theUniversidadAutónoma Institute of Geology the to Dr. Rafael Barboza Gudiño (Director of IN119208 Project grants. We are greatly indebted work This wassupported by DGAPA-PAPIIT marked Tethysian affinity. foraminiferal communityThe andalgae have a is alsodefined. foraminifera environment withagreater variety of semi-restricted aminifera. Another intermediate typicalmiliolidfor with numerousof individuals reduced diversitybut commonly ter association of distinguished bythe El Abrafaciesis a shallow-wa An environment withrestricted circulation from environment. whichare present andeutrophic inadeeper foraminifera and benthicssuchas gavellinellids, pithonellidsand of the latest Cenomanian. 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Mid–late Cenomanian larger benthic foraminifers from the El Abra Formation RESULTS AND DISCUSSION