REVISTA MEXICANA DE CIENCIAS GEOLÓGICAS

v. 39, núm. 1, 2022, p. 71-81

DOI: http://dx.doi.org/10.22201/cgeo.20072902e.2022.1.1672

 

INTRODUCTION

The planktic foraminifera are generally abundant and well preserved in mid-Cretaceous marine sediments; they have been affected during the OAEs (Oceanic Anoxic Events) (Leckie et al., 2002; Premoli Silva et al., 1999; Föllmi, 2012; Kuroyanagi et al., 2020).

The greenhouse climate of the mid-Cretaceous was related to ocean crust output that increased considerably, forming an extensive, thick oceanic plateau named the Large Igneous Provinces (LIPs), including the Ontong Java Plateau (OJP) (early Aptian), the Kerguelen Plateau (late Aptian–early Albian), and the Caribbean Plateau (Cenomanian–Santonian) (Tarduno et al., 1991; Leckie, et al., 2002; Bottini et al., 2015; Erba et al., 2015).

The relationship with OAEs suggests that these submarine volcanic events provoked perturbations in ocean chemistry and fertility, providing nutrients (especially iron) that advance to sulfate reduction in the water column, with the precipitation of pyrite framboids, as well as the deposition of organic matter evolving from a poorly oxygenated stage to an anoxic and finally euxinic stage (Jenkyns, 2010).

The pyrite framboidal structure is one of the important characteristics of anoxic conditions (Wignall et al., 2005) that can be preserved through geologic time. Within the water column, the framboids quickly precipitate, presenting a small average size, while early diagenetic framboids in the sediment present larger sizes (Wilkin et al., 1996).

The Aptian is distinguished by climate changes and extreme environmental perturbations, including OAEs, that represent a global phenomenon of organic-matter burial in oxygen-depleted oceans. In addition to the well-known Selli Event in the early Aptian, Sliter (1989a) recognized a level rich in organic carbon from the Franciscan Complex, California. Later (1999 ), this author used the name “Thalmann Event” for a perturbation of the carbon cycle and placed it between the Globigerinelloides ferreolensis and Gl. algerianus zones of late Aptian age.

In Santa Rosa Canyon (Mexico), Bralower et al. (1999, p. 427) recorded a sharp increase in δ13C org values in the planktic foraminiferal Globigerinelloides algerianus Zone (segment C9) followed by level δ13C org values (segment C10) for the upper parts of the same zone.

Leckie et al. (2002, p. 13) indicated that between OAE1a and OAE1b, a black shale event in the late Aptian within the Globigerinelloides algerianus Zone may be another OAE, as was previously cited by Bralower (op cit).

Friedrich et al. (2003) documented several episodes, among them a black-shale horizon, the “Niveau Fallot 4,” within the Globigerinelloides algerianus Zone in the Vocontian Basin of southern France.

Herrle et al. (2004, fig. 5) record marly black shale horizons from the Mazagan Plateau marked by positive carbon isotope excursion, including the Globigerinelloides algerianus.

Yilmaz (2008) documented black shale-mudstone interval of Upper Aptian that has been recorded within the Globigerinelloides algerianus-Pseudoplanomalina cheniourensis zones in the Deirmenözü section at NW Turkish (fig. 3, p. 288).

Hosseini and Conrad (2010) recorded an interval dated as late Aptian (Gargasian), the Globigerinelloides ferreolensis Zone, which correlates with a major ocean anoxic event (OAE). The occurrence of planktic foraminifers with radial chambers; Leupoldina reicheli, L. pustulans and Hedbergella roblesae, was interpreted as an adaptation to a depleted oxygen environment from a section at west of the Kazerun Faul, throughout the Zagros Fold Belt, SW of Iran.

The objective of this study is to report and describe the planktic foraminifers that are used for dating, moreover we analyzed the planktic foraminifera paleoecology, in addition we infer the depositional environment based on the microfacies, the foraminiferal association and framboidal pyrite occurrence.

 

Geological Setting

During the Early Cretaceous, the Gulf of Mexico basin was tectonically stable except for continuing slow subsidence of its central part, growth faulting of the margins of some depocenters and local deformation related to underlying Jurassic salt. The Lower Cretaceous rocks are carbonates and evaporites on the shelves and carbonates in the bathyal areas (McFarlan and Menes, 1991).

In Mexico, the first Lower Cretaceous investigations of the surface and subsurface were carried out by Heim (1926), followed by Burckhardt (1930), Muir (1936), Imlay (1944), Bodenlos et al. (1956). Since then, there has been a proliferation of litho-stratigraphical terms.

According to Muir (1936) the term Tamaulipas limestone first has been used by Stephenson (1921) in a private study for the Mexican Gulf Oil Company.

Belt (1925) indicated that “the Tamaulipas limestone outcrops typically in the Sierra Tamaulipas and in the first ranges of the Sierra Madre, west of Ciudad Victoria, and is given the name of Tamaulipas on account of its abundant occurrence and typical development in the state of Tamaulipas. It has also been observed in the front ranges of the Sierra Madre from Tamazunchale to a point southeast of Coyutla, Veracruz. The Tamaulipas formation is a fine-grained, compact limestone with well-marked bedding. The uppermost is predominantly gray in color and contains many chert lenses and nodules of irregular shape. The color of the cherts varies from black to almost white. The lower part of the formation consists of creamy to white compact limestone”.

Muir (1936, p. 23) stated that “the Tamaulipas limestone has never been defined in the literature with reference to a definite type locality. It crops out in and forms the main mass of the Sierra de Tamaulipas and is well developed in the Sierra de San Carlos farther north. This facies exists in the front ranges of the Sierra Madre Oriental southeast of Tamazunchale. From Monterrey to Victoria and far south as Gómez Farias it forms the bulk of the front ranges”, but although the name is considered an informal name, it is widely used in the literature. This author shows the subdivision of Tamaulipas limestone in lower and upper divided by the "Otates horizon" as dark rock 20-30 feet thickness, considered as a distinct key horizon markedly different from the white limestone above and below it (p. 38, fig. 8).

According to Longoria (1975, p. 45) the biostratigraphic position of the "Otates limestone member" correspond to Globigerinelloide algerianus Zone of late Aptian age.

Ross and McNulty (1981) indicated that the Tamaulipas limestone is composed of resistant, light gray to black, thin- to thick-bedded wackestone and mudstone in the Sierra de Santa Rosa, Nuevo León. It is about 800 m thick and is delimited at base by the Taraises and the Cuesta del Cura in the top. A medial unit (64 meters) of black, laminated, thin-bedded wackestone permits division of the succession into three parts, for which many different stratigraphic names are applicable. Microfossils are rare to scarce in the lowest unit but are abundant in the medial part and common in the upper unit. The microfauna is pelagic dominated by foraminifers, radiolarians and colomiellids, nannoconids, calcispheres, that are abundant at some levels in the upper unit. Chronostratigraphically useful taxa suggests that all the lower unit of the Tamaulipas is Hauterivian and Barremian. The middle unit is Aptian, and the upper unit is lower Albian.

The Chapulhuacán Limestone was informally defined by Bodenlos et al. (1956, p. 301). This author states that it was previously named “Tenestipa limestone” and described by Heim (1926). It is located NW of Tamazunchale and takes the name of the village Chapulhuacán located on Federal Highway 85, and its lithology may be comparable to the lower Tamaulipas limestone referred to by Muir (1936).

 

MATERIAL AND METHODS

The samples were collected from the Cerro Boludo locality (Figure 1), which is located at the north of the state of Hidalgo, at kilometer 250 of Federal Highway 85 (Mexico–Laredo), between the towns of Chapulhuacán and Tamazunchale. The outcrops are located at 21º 11.742' N and 98º 54.333' W. The section has a reduced thickness of approximately 20 m. consisting of black marly limestone of medium thickness, with intercalations of shale in thin layers (Figure 2).

For micropaleontological and microfacies analysis the samples were prepared in thin sections 50 µm thick, obtaining axial and equatorial sections of the planktic foraminifera. The identification of the species in thin section is based on the papers of Sliter (1989b; 1992) and Premoli Silva and Verga (2004). The age assignment follows the zonation proposed by Premoli Silva and Verga (2004) and Coccioni (2020).

Pyrite framboids were observed in thin sections using a reflected-light Olympus BX-60 microscope at magnifications of 50x and 100x and a low-vacuum Hitachi TM-1000 table-top scanning electron microscope (SEM).

 

RESULTS

Biostratigraphy

The biostratigraphic significance of planktic foraminifera is widely recognized, as they are a valuable tool in dating, so they permit us to determine the age of the samples studied from the Cerro Boludo locality.

Based on the planktic foraminiferal assemblage we record the Globigerinelloides algerianus Total Range Zone.

 

Globigerinelloides algerianus Total Range Zone

Author : Moullade, 1966.

Definition: Total range of the nominate taxon.

Remarks: This zone is characterized by an assemblage composed of common to abundant large taxa as Globigerinelloides algerianus Cushman and ten Dam, 1948, G. barri (Bolli, Loeblich and Tappan, 1957), moreover G. ferreolensis (Moullade, 1961), G. aptiensis Longoria,1974, G. blowi (Bolli, 1959), Pseudoplanomalina cheniourensis (Sigal, 1952), as well as Hedbergella roblesae (Obregón de la Parra, 1959),

H. occulta Longoria, 1974, H. luterbacheri Longoria, 1974 and H. similis Longoria, 1974 (Figures 3, 4).

Age. According to the zonal schema for tropical regions (Caron, 1985; Premoli Silva and Sliter, 1995; Robaszynski and Caron 1995; Premoli Silva and Verga, 2004), the age assigned to the zone is late Aptian, however recently, Coccioni (2020, p. 288) refined the assignment age and he gave an early late Aptian to middle late Aptian to this interval.

 

Paleoecology and Paleoenvironment

Microfacies

Microfacies 1- Pelagic foraminiferal-radiolarian wackestone (Sample CB-1 and 1a); the components of the microfacies are planktic foraminifers such as globigerinelloids, and hedbergellids with elongated chambers. The radiolarians are common. The foraminiferal chambers are filled with pyrite. Organic matter is uniformly distributed in the micritic matrix and contain framboids (Figure 5a).

Microfacies 2- Planktic Foraminiferal wackestone (Sample CB-2); laminated organic matter is intercalated with the micrite with abundant skeletal grains of planktic foraminifers and radiolarians. Fabric of this microfacies is mud-supported. (Figure 5b).

Microfacies 3- Foraminiferal wackestone-packstone (Sample CB-4); with abundant of planktic foraminifers and radiolarians preserved in micrite. The main characteristic of this microfacies is the gross bed of laminated organic matter containing framboids (Figure 5c)

Microfacies 4- Foraminiferal-radiolarian wackestone (Sample CB-6); this microfacies is defined by a mixed micrite and organic matter and the planktic foraminiferal association with gobigerinelloids, hedbergellids, as well as benthic foraminifera (Figure 5d).

Framboids are the most common form of pyrite in the studied samples. They occur randomly distributed in the micritic matrix and within intra-skeletal pores, as single framboids and clusters of framboids. Individual pyrite framboids are generally < 8 μm (Figure 6a, 6b, 6c).

The distribution of planktic foraminifera is controlled by conditions such their position in the water column, which is likely to be most critical. Test morphologies may function in relation to the density of the foraminifera and its difference from water, as well as resistance to sinking and turbulence. These foraminifera probably utilize different feeding, reproductive, behavioral, and life history strategies in eutrophic and oligotrophic waters (Lipps, 1979).

Other environmental factors, such as temperature, stratification, light intensity, and food availability affect the growth and distribution of the individual planktonic foraminifera (Schiebel et al., 2001; Žaric et al., 2005; Kretschmer et al., 2018).

We documented the depth ecology of some planktic foraminifera observed in the studied interval.

The genus Hedbergella is opportunist or r/strategist with varied depth habitats and an affinity for eutrophic conditions, probably adapted to changes in temperature, salinity, nutrients, and oxygen inhabiting the near-surface waters, likely depending on primary productivity (Premoli Silva and Sliter, 1999). Thus, Aptian hedbergellids may have been able to change habitats in the water column and tolerate wide environmental variations (Hart, 1999; Price and Hart, 2002).

The planktic foraminifera with radially elongate chambers such as Hedbergella roblesae and H. similis indicate an adaptive response to oxygen depletion (Magniez-Jannin, 1998; Premoli Silva and Sliter, 1999; Coccioni et al., 2006).

The Globigerinelloides species are regarded as the most specialized r/k strategists, possibly mesotrophic forms during the Aptian interval (Coccioni, Erba and Premoli Silva, 1992; Premoli Silva and Sliter, 1999).

Based on the textural features characteristics, we identify the Standard Microfacies (SMF 3-For) (Flügel, 2010) corresponding to pelagic deep-water basinal facies (FZ 1) of Wilson (1975). In addition, the foraminiferal assemblage and the microlaminated fine-grained texture with organic matter and framboids of pyrite, indicate a pelagic deep-water oxygen-deficient environment in the Globigerinelloides algerianus Total Range Zone in the late Aptian. In addition, the presence of radiolarians indicates ocean eutrophication.

 

DISCUSSION

The name “Tamaulipas limestone” was employed by Stephenson (1921, in Muir 1936) in a private report for the Mexican Gulf Oil Company. Subsequently Belt (1925) stated that the lower limit of this unit was not observed by him, but that the San Felipe beds overly it with a marked lithological change but without evidence of angular disconformity.

Muir (1936) illustrated a tripartite division for the Tamaulipas limestone in lower and upper Tamaulipas. The Otates horizon is in the middle part.

The Tamaulipas limestone is widely distributed, typically in the Sierra de Tamaulipas and the front ranges of the Sierra Madre in northeastern Mexico. It has been studied by several authors, Humphrey and Diaz (1956) , Carrillo Bravo (1961), Enos (1974), Longoria (1975), Gamper (1977), and Chavez Cabello et al. (2011).

Ross and McNulty (1981) studied the microfossils dating the Tamaulipas limestone, from the Hauterivian to Albian in the Santa Rosa Canyon, Sierra Madre Oriental, Nuevo León.

In the study of the Tamaulipas limestone outcropping in the Cerro Boludo locality in northern Hidalgo state, we identified for the first time the Globigerinelloides algerianus Total Range Zone, based on the stratigraphic distribution of the planktic foraminifera.

Age assignment for this interval is early late Aptian to middle late Aptian according to Coccioni (2020) in the recent zonal scheme proposed for the Tethys Realm.

This zone has been recorded in Mexico; for instance, in the Santa Rosa Canyon, Nuevo León (Longoria, 1975, 1984; Ross and McNulty, 1981; Bralower et al., 1999) and in the Sierra de Parras (Lehmann et al., 1999, p. 1018).

For the paleoenvironmental interpretation, the microfacies analysis and the foraminiferal assemblage for the Globigerinelloides algerianus Total Range Zone from the “Otates horizon” indicate that the deposit took place in a pelagic deep-water environment in the studied locality.

In this zone, the presence of planktic foraminifera with elongated chambers, adapted to stressed conditions which are frequently found in deposits with organic matter is interpreted as an adaptation to low oxygen levels in the upper water column (Premoli Silva et al., 1999; Coccioni et al., 2006).

Moreover, the occurrence of radiolarians and pyrite framboids, as well as an increasing supply of nutrients, suggests oxygen depletion in the paleoenvironment recognized during the Aptian and related to an anoxic event reported in this interval (Bralower et al.,1999; Leckie et al., 2002; Khan et al., 2021).

The anoxic conditions during the Globigerinelloides algerianus Zone revealed in this research are the local expression of the so called “late Aptian anoxic event” first reported by Bralower et al. (1999) in the Santa Rosa Canyon section, NE Mexico. There corresponds to an organic-rich interval. This event has been also identified by Kochhann et al. (2013) in cores 42-39 at DSDP Site 364 (South Atlantic Ocean), associated to the occurrence of black shale levels or even with the conditions that led to the formation of the Niveau Fallot 4 in the Vocontian basin (SE France; Friedrich et al., 2003; Herrle et al., 2004), and the black-shale-mudstone interval identified at NW Iran (Yilmaz, 2008) , also the studied succession could be correlate in part with the Thalmann Event identified in the San Francisco Complex of northern California, USA (Sliter, 1989a;1999).

Radiolarian-rich facies within the Globigerinelloides algerianus Zone have also been recently documented by Gutiérrez-Puente et al. (2021) in the Linderos section, central eastern Mexico, which reinforce the idea of upwelling along the western margin of the Gulf of Mexico during Aptian time.

 

SYSTEMATIC PALEONTOLOGY

The species identified in this study are described and the synonymies are constrained to the references applicable to knowledge on the foraminifera in thin sections. The thin sections are housed in the Paleontology Collection of the Institute of Geology (Universidad Nacional Autónoma de México). The stratigraphic range of the described species has been transcribed from pforams@mikrotax.

Supergroup Rhizaria Cavalier-Smith, 2002

Class Foraminifera d’Orbigny, 1826

Order Globigerinina Delage and Hérouard, 1896

Family Globigerinelloididae Longoria, 1974

Subfamily Globigerinelloidinae Longoria, 1974

Genus Globigerinelloides Cushman and ten Dam, 1948

Type species. Globigerinelloides algerianus Cushman and ten Dam, 1948.

 

Globigerinelloides algerianus Cushman and Ten Dam, 1948 (Figure 3a, 3b, 3d, 3e)

Globigerinelloides algeriana Cushman and Ten Dam, 1948, p. 43, pl. 8, figs 4–6; Sliter, 1989b, p. 13, pl. 1, figs. 13-14; Sliter, 1992, p. 288, fig. 6 (1); Sliter, 1999, p. 334, pl. 2, figs. 17-18; Premoli Silva and Verga, 2004, p. 324, pl. 157, figs. 13-14; Mandic and Lukeneder, 2008, p. 906, fig. 7 (9).

Description. Test large, planispirally coiled, periphery broadly rounded; chambers globular, 10-12 in last whorl, increasing gradually and evenly in size as added; sutures depressed, in the earlier stages nearly radial, later somewhat arched; wall calcareous, finely perforate, the surface relatively rugose, showing dark and light layers in thin section; aperture a small, arched opening in the median line at the base of the apertural face.

Stratigraphic range. First and last occurrence in the G. algerianus Zone (Aptian stage).

 

Globigerinelloides aptiensis Longoria, 1974 (Figure 3j)

Globigerinelloides aptiense Longoria, 1974, p. 79, pl. 4, figs. 9–10, pl. 8, figs. 4–6, 17, 18. Globigerinelloides aptiensis; Sliter, 1999, p. 334, pl. 2, figs. 8-9; Premoli-Silva and Verga, 2004, p. 239, pl. 9, fig. 6; Blowiella aptiensis (Longoria) Mandic and Lukeneder, 2008, p. 906, fig. 7(5).

Description. Test small, planispiral, biumbilicate, peripheral outline subcircular lobate, with five to six globular chambers in the last whorl increasing gradually in size as added, sutures radial and depressed; relict apertures and flaps could be observed.

Remarks. Globigerinelloides aptiensis differs from Globigerinelloides blowi by having more numerous chambers in the last whorl and slow growth rate resulting in a lobate test. The spiral view of the specimen observed is comparable to the illustration of Premoli-Silva and Verga (2004).

Stratigraphic range. First occurrence within Globigerinelloides blowi (base in Barremian stage); last occurrence within Paraticinella rohri (top in Aptian stage).

 

Globigerinelloides barri (Bolli, Loeblich and Tappan, 1957) (Figures 3g, 3h)

Biglobigerinella barri Bolli, Loeblich and Tappan, 1957, p. 25, pl.1, figs. 13-18; Globigerinelloides barri (Bolli, Loeblich and Tappan); Longoria,1974, p. 80-82, pl.4, figs. 1-3, 8, 14, pl. 5, figs. 9-16; Sliter, 1992, p. 288, fig. 6(2); Sliter, 1999, p. 334, pl. 2, fig. 20; Mandic and Lukeneder, 2008, p. 906, fig. 7(10).

Description. Test planispiral, biumbilicate, nearly involute to evolute; peripheral margin somewhat lobulate; chambers ovate to nearly spherical; in some specimens a smaller low but broad final chamber may cover a double-apertured penultimate chamber or there may be a small chamber at each side of the periphery; wall calcareous, finely perforate, surface distinctly rugose; aperture equatorial, a low arch bordered above with a narrow lip; in the later stage there is a double aperture consisting of a small extraumbilical arch at each side of the last chamber, or one to each of the final paired chambers which may extend almost into the umbilicus.

Stratigraphic range. First occurrence within Globigerinelloides blowi Zone (base in the Barremian stage); last occurrence within G. algerianus Zone (top in Aptian stage).

 

Globigerinelloides ferreolensis (Moullade, 1961) (Figures 3c, 3f)

Biticinella ferreolensis Moullade, 1961, p. 214, pl. 1, figs 1–5. Globigerinelloides ferreolensis (Moullade) Moullade, 1966, p. 123, pl. 9, figs. 1–3; Sliter, 1989b, p. 13, pl. 1, figs. 11, 12; Sliter, 1992, p. 288, figs. 6 (5,6); Sliter, 1999, p. 334, pl. 2, fig. 19; Premoli Silva and Verga, 2004, p. 239, pl. 9, figs. 12-15; Mandic and Lukeneder, 2008, p. 906, fig. 7 (7).

Description. Planispiral test, perforate, slightly compressed, chambers increasing in size gradually from small chambers in early whorls and larger chambers in final whorl, with 7-9 globular chambers; wall relatively thick.

Stratigraphic range. First occurrence within Leupoldina cabri Zone (base in the Aptian stage); last occurrence within Ticinella bejaouaensis Zone (top in Aptian stage).

Family Planomalinidae Bolli, Loeblich and Tappan, 1957

Genus Pseudoplanomalina Moullade, Bellier, Tronchetti, 2002

Type species. Planulina cheniourensis Sigal, 1952.

 

Pseudoplanomalina cheniourensis (Sigal, 1952) (Figures 4a, 4b)

Planulina cheniourensis Sigal 1952, p. 20, fig. 17): Sliter, 1992; p. 288, fig, 6 (10-11); Sliter, 1999, p. 334, pl. 2, fig. 27; Pseudoplanomalina cheniourensis (Sigal) Moullade, et al., 2002, p. 130- 131, fig. 3; Premoli Silva and Verga, 2004, p. 264, pl. 34, figs. 1-5.

Description. Test compressed planispiral, bi-evolute, with typically diamond-shaped chambers and angular profile in transverse section with a distinct break in the peripheral round, better marked on the first chambers of the last whorl forming a peripheral pseudo-keel.

Stratigraphic range. First occurrence within Leupoldina cabri Zone (base in the Aptian stage); last occurrence within Hedbergella planispira Zone (top in Albian stage).

Family Hedbergellidae Loeblich and Tappan, 1961

Subfamily Hedbergellinae Loeblich and Tappan, 1961

Genus Hedbergella Brönnimann and Brown, 1958.

Type species. Anomalina lorneiana d'Orbigny var. trochoidea Gandolfi, 1942.

 

Hedbergella luterbacheri Longoria, 1974 (Figure 3k)

Hedbergella luterbacheri Longoria, 1974, p. 61, pl.19, figs. 21-23, 24-26; pl. 26, figs. 15-17; Premoli-Silva and Verga, 2004, p. 239, pl. 9, fig. 6 

Description. Medium-sized, test coiled in a low trochospire, formed by about 3 whorls, peripheral margin circular, chambers spherical in axial view; umbilicus wide.

Stratigraphic range. First occurrence within Hedbergella similis Zone (base in Barremian stage); last occurrence within Globigerinelloides algerianus Zone (top in Aptian stage).

 

Hedbergella roblesae (Obregón de la Parra, 1959) (Figure 4c)

Globigerina roblesae Obregón de la Parra, 1959 , p. 149, pl. 4, fig. 4. Hedbergella roblesae (Obregón de la Parra) Longoria, 1974, p. 65, pl. 16, figs 1–6; pl. 20, figs 10, 11; Premoli Silva and Verga, 2004, p. 251, pl. 21, figs. 6-8; Clavihedbergella roblesae (Obregón de la Parra), Sliter, 1999, p. 335, pl. 3, figs. 7-8.

Description. Trochospiral test, the peripheral margin is lobate; spiral side low to medium-high; the first chambers are globular, the last 3 are elongate; sutures straight on spiral side; the wall texture is calcareous, finely perforated, smooth.

Stratigraphic range. First occurrence within Hedbergella similis Zone (in Barremian stage); last occurrence within Globigerinelloides algerianus Zone (top in Aptian stage).

 

Hedbergella similis Longoria, 1974 (Figure 4d)

Hedbergella similis Longoria, 1974, p. 68, pl. 16, figs. 10–21, pl. 18, figs. 12, 13, pl. 23, figs. 14–16; Sliter, 1992, p. 290, fig. 7(6-7); Sliter, 1999, p. 335, pl. 3, figs. 6, 13.

Description. Test small to medium trochospirally coiled, with 2–3 whorls composed of five to six chambers in the last whorl globular then elongate, gradually increasing in size; peripheral margin lobate, sutures radial, slightly curved, on both umbilical and spiral sides; sutures radial, slightly curved, relict apertures commonly observed on spiral side.

Remarks. Hedbergella similis is differentiated from Hedbergella semielongata by having a depressed inner spire and more chambers in the last whorl.

Stratigraphic range. First occurrence within Hedbergella similis Zone (base in Barremian stage); last occurrence within Globigerinelloides algerianus Zone (top in Aptian stage).

 

Hedbergella semielongata Longoria,1974 (Figure 4e)

Hedbergella semielongata Longoria, 1974, Longoria, 1974, p. 66, pl. 20, figs. 12-13, pl. 21, figs. 1-3, 4-5; Premoli Silva and Verga, 2004, p. 251, pl. 21, figs. 9-10.); Clavihedbergella semielongata Sliter,1999, p. 335, pl. 3, fig. 12.

Description. Test trochospirally coiled; 4 chambers in the outer whorl, chambers firstly globular to subglobular, the last two radially elongate; spiral side relatively high; peripheral outline cross-shaped; sutures straight to slightly curved on both spiral and umbilical sides. Stratigraphic range. First occurrence (base) within H. similis Zone (base in Barremian stage); last occurrence (top) within G. algerianus Zone (top in Aptian stage). Wall smooth and finely perforate.

 

Hedbergella occulta Longoria, 1974 (Figure 4f)

Hedbergella occulta Longoria, 1974, p. 63, 64, pl. 11, figs. 1–3, 7, 8, pl. 20, figs. 5–7, 8, 9, 17, 18; Premoli-Silva and Verga, 2004, p. 251, pl. 21, fig. 3; Praehedbergella occulta Mandic and Lukeneder, 2008, p. 906, fig. 7(11).

Description. Test medium in size, coiled in a low to moderate trochospire, chambers globular, somewhat ovoid on both spiral and umbilical sides; spherical in peripheral view; sutures radial, slightly curved on both spiral and umbilical sides; umbilicus circular, deep.

Stratigraphic range. First occurrence within Globigerinelloides blowi Zone (base in the Aptian stage); last occurrence within Ticinella bejaouaensis Zone (top in Aptian stage).

 

CONCLUSIONS

We identified and described in thin section the most important species of planktic foraminifera included in the studied samples from Cerro Boludo, Hidalgo.

Based on the foraminiferal assemblage, the Globigerinelloides algerianus Total Range Zone of the early late-middle late Aptian age was recognized.

The studied dark marly limestone samples of wackestone texture contain an assemblage characterized by planktic foraminifera suggesting a pelagic open-marine environment. Moreover, presence of pyrite framboids and the organic matter deposit indicate depleted oxygen conditions which correlate with the local anoxic events described in other locations that took place during the late Aptian.

 

ACKNOWLEDGEMENTS

The authors wish to acknowledge the Instituto de Geología of the Universidad Nacional Autónoma de México for supporting this study. We thankful to Dra. Ana Bertha Villaseñor (UNAM) for providing the samples and the information of the locality.We thank to the anonymous reviewer and Dr. Carmen Rosales (Independent Research) for their useful comments and remarks that much improved the manuscript.We are deeply grateful to the Editor in Chief Dr. Angel F. Nieto Samaniego (Centro de Geociencias, UNAM, Mexico) for his careful handling of our paper. We thank to Ing. J Jesús Silva Corona Technical Editor (Centro de Geociencias, UNAM Juriquilla, México) for the final review of the manuscript.

 

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