Acritarchs of the Ediacaran Frecheirinha Formation, Ubajara Group, Northeastern Brazil

Chiglino, Leticia; Gaucher, Claudio; Sial, Alcides N.; Ferreira, Valderez P.

doi:10.1590/0001-3765201520140430

Abstract

We report for the first time the occurrence of organic-walled microfossils in Ediacaran limestones and marls of the Frecheirinha Formation, Ubajara Group, and the first Precambrian acritarchs so far reported for northeastern Brazil. The assemblage of the Frecheirinha Formation represents a low-diversity microflora comprising Leiosphaeridia, Lophosphaeridium and subordinated Bavlinella (=Sphaerocongregus). Their thermal alteration index (TAI) between 4+ and 5, suggests metamorphic temperatures exceeding 200-250°C. Higher temperatures are probably related to intruding granitic plutons (Meruoca, Mucambo). Reported δ13C values of carbonates of -3.5 ‰ VPDB (Vienna-Peedee Belemnite) at the base, passing up section into a positive plateau of up to +3.7 ‰, and corresponding 87Sr/86Sr values between 0.7075 and 0.7080 suggest an Ediacaran age. The acritarch assemblage is comparable to the Late Ediacaran Leiosphere Palynoflora (LELP) or Kotlin-Rovno assemblage, in broad agreement with chemostratigraphic data. Macrofossils belonging to the Ediacara fauna were reported from the overlying Jaibaras Group, which would constrain even further the depositional age of the Frecheirinha Formation to within ca. 575-555 Ma. A more comprehensive palynological study of the Frecheirinha Formation is necessary to confirm this age assignment.

Acritarchs; Ediacaran; Neoproterozoic; northeastern Brazil

INTRODUCTION

The Neoproterozoic is characterized by extreme climate change, oscillations in oceanic geo chemistry, a significant oxygenation event, and the diversification of the marine biota (Hoffman and Schrag 2002, Willman et al. 2006, Frei et al. 2009, Halverson et al. 2010). Several near-global glacial events ocurred between 740 and 580 Ma, considered as a bottleneck for marine biota evolution (Kaufman and Knoll 1995, Moczydłowska 2008).

Neoproterozoic body fossils have been described for a few successions in Brazil, the most diverse being the assemblage preserved in the late Ediacaran Corumbá Group, Mato Grosso do Sul (e.g. Beurlen and Sommer 1957, Zaine and Fairchild 1985, Gaucher et al. 2003, Fairchild et al. 2012 Warren et al. 2012).

Until recently, no Neoproterozoic body fossils were known from northeastern Brazil. Soft-bodied macrofossils typical of the Ediacara Fauna, which can be assigned to the White Sea assemblage (Narbonne 2005), were recently described from the Jaibaras Group, Ceará (Barroso et al. 2014, Figs. 1-2). The Jaibaras Group overlies the Ubajara Group (Fig. 2), which comprises thick carbonates rocks of the Frecheirinha Formation, with an erosional unconformity between the two groups. The Ubajara Group represents a proximal platform sequence, composed, from base to top, of the following formations (Fig. 2a): (a) Trapiá (quartz conglomerate), (b) Caiçara (ferruginous siltstones), (c) Frecheirinha (limestones and subordinate marls) and (d) Coreaú (sandstone and greywacke) located in the Médio Coreaú Domain, Borborema Province. This Domain is characterized by graben and horst structures controlled by NE-trending shear zones, and is bounded to the northeast by the Transbrasiliano Lineament, which separates it from the Ceará Central Domain (Caby et al. 1991, Santos et al. 2008). The age of the carbonate rocks of the Frecheirinha Formation is poorly constrained by C- and Sr-chemostratigraphy and radiometric ages as late Neoproterozoic (Sial et al. 2000, 2003, Chiglino 2013).

Fig. 1
Geological map of the studied area, showing the Ubajara Group and sampled outcrops of the Frecheirinha Formation (Araticum Section).

Fig. 2
Lithostratigraphy of the Ubajara and Jaibaras groups, showing stratigraphic range of fossils occurring in these units. a-Chemostratigraphy (δ13C and 87Sr/86Sr) of the entire Frecheirinha Formation (Sial et al. 2003, Chiglino 2013). b-Detail of the stratigraphic interval sampled in this work.

In the present work, we describe organic-walled microfossils (acritarchs) from the Frecheirinha Formation, which contribute towards our under standing of the depositional environments, age and thermal overprint of the Ubajara Group. These are the first Precambrian acritarchs reported, so far, from northeastern Brazil.

LITHOSTRATIGRAPHY AND AGE

The Ubajara Group represents a proximal platform sequence (Costa et al. 1979, Hackspacher et al. 1988), the type area is located along the road BR 222 between Aprazível and Saco towns, roughly 300 km from the city of Fortaleza (state of Ceará; Fig. 1). This sedimentary succession reaches 3000 m in thickness and is composed, from base to top, by:

(a) Trapiá Formation sandstones.

(b) Caiçaras Formation, fine-grained sandstones which pass into red, finely laminated siltstones up section.

(c) Frecheirinha Formation, pink and dark gray limestones and subordinated marls at the base and gray limestones with microbial lamination at the top.

(d) Coreaú Formation, sandstones and graywackes.

The contact between the base of the Ubajara Group and the basement is not exposed, and at the top it is overlain by the Jaibaras Group with erosional unconformity (Oliveira 2000, Santos et al. 2008).

The Frecheirinha Formation is a carbonate unit about 500 m in thickness, the type area is located near the Frecheirinha town and the best exposures are observed at the quarry of the Companhia Cearense de Cemento Portland (CCCP), north of Aprazível. The strata exhibit intense ductile deformation recorded by folds with axes oriented NE-SW and, locally, low grade metamorphism.

Carbonates are characterized by limestones and marly rythmites in the lower part, which pass into dark gray to gray, fine, laminated, stromatolitic limestones at the top. In the Araticum area (Fig. 1), carbonates are composed of fine-grained, calcitic mudstones (grain size: 10 µm; Figs. 3a-b) intercalated with organic-rich marls (Fig. 3a), in which microfossils are preserved. On the other hand, in the Angustura farm region recrystallization of carbonates is evident, and the occurrence of tremolite in the limestones (Figs. 3c-d) indicates that they reached low-grade metamorphic conditions. This metamorphism was probably caused by the nearby Mucambo Granite (Fig. 1) and is not regional in nature.

Fig. 3
Microphotographs of thin sections of carbonates of the Frecheirinha Formation. a-Contact between calcitic mudstone (below) and organic-rich marl, Araticum section, crossed nicols. b-Stylolite in fine-grained limestone (Araticum section), plane-polarized light. c-Recrystallized limestone (marble) from the Angustura section, plane-polarized light. Note tremolite crystals. d-Same as previous, crossed nicols.

The Araticum profile, located between the Frecheirinha and the Ubajara village (Fig.1), was selected for the palynological study because of the lower thermal overprint. There, limestone-marl rhythmites occur at the base, which grade into dark gray to black, finely laminated, organic-rich limestones at the top (Fig. 2).

Barroso et al. (2014) reported the occurrence of probable soft-bodied Ediacaran macrofossils in the overlying Jaibaras Group, similar to the White Sea assemblage, which justify an Ediacaran age for this unit (560-542 Ma: Narbonne 2005, Fedonkin et al. 2007). These biostratigraphic relationships may provide a minimum late Ediacaran age constraint for the Frecheirinha Formation, but it needs a more detailed study to explore the paleontological affinity of the macrofossils described by Barroso et al. (2014) and their relationship to the Ediacara fauna.

The age of the Ubajara Group is still uncertain due to the lack of reliable radiometric ages. The minimum age is constrained by the following ages:

(a) a Rb-Sr age of 562 ± 19 Ma determined for the Coreaú dike swarm, which crosscuts the sequence (Sial and Long 1987),

(b) the Mucambo Granite intrudes the Ubajara Group (Fig. 1) and yielded a U-Pb crystallization age of 532 ± 7 Ma (Santos et al. 2008), and

(c) a Rb-Sr age of 540 ± 24 Ma, a U-Pb age of 532 ± 24 Ma (Fetter et al. 2003) and a U-Pb SHRIMP age of 541 ± 5 Ma (Santos et al. 2013) for the Meruoca Granite, which intrudes the group and develops an important contact aureole. The U-Pb SHRIMP age of 541 Ma is considered the best age estimate for the crystallization of the pluton.

Chemostratigraphic data presented by Chiglino (2013, Fig. 2 a and b) show negative δ¹³C values of -3.5‰ VPDB at the base, passing up section into a positive excursion with maximum values of +3.7‰. Corresponding ⁸⁷Sr/⁸⁶Sr values range between 0.7075 and 0.7080 (Sial et al. 2003). Especially the Sr isotope ratios, which were obtained from high-Sr limestones (Sr concentration up to 3500 ppm: Chiglino 2013), favor a latest Cryogenian to Ediacaran depositional age (e.g. Jacobsen and Kaufman 1999, Melezhik et al. 2001, Halverson et al. 2007). However, late Cryogenian successions are often characterized by elevated δ¹³C values of up to +8‰ VPDB which drop to negative values before the end-Cryogenian glaciation (Halverson et al. 2005). This pattern is not observed in the Frecheirinha Formation. Instead, a plateau around +3‰ VPDB characterizes most of the unit and post-dates a negative excursion, similar to that observed for the late Ediacaran Nama and Corumbá groups (Grotzinger et al. 1995, Boggiani et al. 2010; Table I). Likewise, a negative excursion followed by moderately positive values is also observed in the late Ediacaran upper Polanco Formation (Arroyo del Soldado Group, Uruguay), which is also associated to ⁸⁷Sr/⁸⁶Sr values between 0.7070 and 0.7082 (Gaucher et al. 2009, Frei et al. 2011). Thus, the chemostratigraphic data suggest an Ediacaran age as the most probable depositional age of the Frecheirinha Formation, but so far do not allow a more refined geochronology.

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TABLE I
Table showing key correlation features for several Neoproterozoic units dominated by Bavlinella and/or Leiosphaeridia. Features shown include radiochronometric constraints (mainly U-Pb), δ13C, 87Sr/86Sr and relative. Sources of data: 1: Chiglino 2013 and this work. 2: Germs et al. (1986) , Grotzinger et al. (1995) . 3: Gaucher (2000) , Gaucher and Poiré (2009) , Gaucher et al. (2009) , Blanco et al. (2009) . 4: Gaucher et al. (2003) , Boggiani et al. (2010) . 5: Mallmann et al. (2007) , Gaucher et al. (2008) , Oyhantçabal et al. (2009) . 6: Grey (2005) , Walter et al. (2000) , Kendall et al. (2006) . 7: Yin and Yuan (2007) , Zhang et al. (2008) . 8: Germs et al. (2009) , Halverson et al. (2005) , Hoffman et al. (1996) , Hoffmann et al. (2004) . 9: Nagy et al. (2009) , Karlstrom et al. (2000) .

MATERIALS AND METHODS

Palynological macerations of carbonates were prepared at the Micropaleontology Laboratory of the Departamento de Geología, Facultad de Ciencias (Montevideo). The method does not use centrifugation or ultrasonic bath to avoid breakage of fragile specimens (e.g. Gaucher et al. 2008). Following crushing and digestion of samples with concentrated HCl, 72% HF was applied for 24h. After neutralization, boiling HCl was applied to remove fluorides formed in the previous step. The remaining solution was diluted with water and the supernatant discarded after allowing at least 30 min for particle settling. The organic residues were recovered by means of a 5 μm sieve, stored in glass flasks and mounted with glycerin-gelatine on standard glass slides. Microfossils were determined under a Leica DM LP polarizing microscope, using both transmitted and reflected light (Pflug and Reitz 1992).

Twelve samples of carbonates and marls of the Frecheirinha Formation at the Araticum section were analyzed. Acritarch preservation was quite poor, mainly due to advanced carbonization, corrosion and fragmentation. Despite the advanced thermal alteration of acritarchs, they could still be classified using reflected light techniques described by Pflug and Reitz (1992) .

RESULTS

PRESERVATION AND THERMAL ALTERATION

Although entire, fairly well-preserved specimens are common, most of the organic remains are fragmentary and/or corroded to some degree. Moreover, acritarchs exhibit advanced carbonization, showing colors from dark gray to black (Figs. 4-6). Corresponding Thermal Alteration Index (TAI) ranges from 4+ to 5, suggesting metamorphic temperatures exceeding 200-250°C (Teichmüller et al. 1998). It is not yet clear if this metamorphic overprint is of a regional nature or enhanced by the voluminous granitic intrusions affecting the succesion, such as the Meruoca and Mucambo granites (Fig. 1). As we have shown in Figs. 3c-d, contact metamorphism is evident in the Angustrura section near the Mucambo Granite (Fig. 1), but it is uncertain as to how far away from the pluton's edge this thermal overprint reaches.

Fig. 4
Sphaeromorphs of the Frecheirinha Formation recovered from limestones (Araticum Section) by means of standard palynological maceration. a- Leiosphaeridia tenuissimaEisenack (1958) , specimen Arat 29A-1, b-L. tenuissimaEisenack (1958) , specimen Arat 29E-9, c-L. tenuissimaEisenack (1958) , specimen Arat 29E-7.

Fig. 5
a- Leiosphaeridia minutissima Naumova (1949) , specimen Arat 29A-5, b- Leiosphaeridia jacutica (Timofeev 1966), specimen ARAT 29E-8, c- Lophosphaeridium sp, specimen 110227/2B-2.

Fig. 6
a-Thin section of limestone (Araticum section) showing hematized Bavlinella faveolata (Schepeleva) Vidal (1976) , specimen ARAT 30 (arrowed), b-Bavlinella faveolata from a palynological maceration of black limestone, specimen ARAT 29C-8 in transmitted light (left) and in combined reflected-transmitted light (right), showing individual microspheres.

Although the advanced carbonization of acrit archs hinders, to some extent, their identification, the use of reflected light techniques allows overcoming this dificculties. Thus, the low diver sity observed in the Frecheirinha microflora is considered as a primary feature, and not the result of a taphonomic bias.

SYSTEMATIC PALAEONTOLOGY

Repository. All palynological slides, containing specimens described here, are kept in the Precambrian collection of the Departamento de Paleontología, Facultad de Ciencias (Montevideo, Uruguay). The position of specimens on the slides are clearly marked on corresponding duplicates.

Incertae sedis

Group Acritarcha Evitt (1963)

Genus LeiosphaeridiaEisenack (1958) , emend. Downie and Sarjeant (1963) , emend. Turner (1984).

Type species: Leiosphaeridia balticaEisenack (1958)

Leiosphaeridia tenuissima Eisenack (1958)

Figs. 4 a-c

1958 Leiosphaeridia tenuissima Eisenack: pl. 1.2-1.3

1994 Leiosphaeridia tenuissima Butterfield et al.: Fig. 16I

1996 Leiosphaeridia tenuissima Hofmann and Jackson: figs. 12E

1998 Leiosphaeridia tenuissima Gaucher et al.: Fig. 4.6

2000 Leiosphaeridia tenuissima Gaucher: pl. 11.5

2004b Leiosphaeridia tenuissima Gaucher et al.: Fig. 4D

2005a Leiosphaeridia tenuissima Gaucher et al.: Fig. 8g-h

2006 Leiosphaeridia tenuissima Gaucher and Germs: figs. 7 d, f-g; 8 b-f

2008 Leiosphaeridia tenuissima Gaucher et al.: figs. 3B-I

Material. Slides Arat 29A-1, Arat 29E-7 and Arat 29E-9. Ten fairly well-preserved specimens and fragments in macerations of carbonates, Frecheirinha Formation.

Description. Thin-walled, psilate, originally spheroidal vesicles with common folds. Diameter ranging between 70 and 100 µm (mean=84 µm; N=5). Two different patterns of folding of the walls were observed in the vesicles: (a) simple, psilate sphaeromorphs with mainly concentric folds (Fig. 4.a); and (b) vesicles with a microplicate wall (Figs. 4.b, c).

Remarks. L. tenuissima is the most frequent species in the black limestones of the Araticum section, and represents the base of the Frecherinha Formation. Two different wall structures are included here under L. tenuissima: one with a thin, but still competent wall, the other with a very thin, pliable membrane. The same wall structure has been observed in specimens from other Ediacaran units in South America: Las Ventanas Formation of Uruguay (Gaucher et al. 2008), and the Sierras Bayas Group of Argentina (Gaucher et al. 2005b).

Leiosphaeridia minutissimaNaumova (1949) , emend. Jankauskas et al. (1989)

Fig. 5a

1992 Leiosphaeridia minutissima Butterfield and Chandler: figs. 3A-3I

1996 Leiosphaeridia minutissima Hofmann and Jackson: figs. 15.9-15.15, 15.16

1996 Leiosphaeridia minutissima Hofmann and Jackson: figs. 12A-C

2000 Leiosphaeridia minutissima Gaucher: p. 66

2008 Leiosphaeridia minutissima Gaucher et al.: Fig. 3A

Material. Slides ARAT 20B, 29A-5, 29B, 34A and 35A, few specimens and vesicle-fragments in palynological macerations of carbonates, Frecheirinha Formation.

Description. Thin-walled and psilate, originally spheroidal vesicles with common, irregular to concentric folds. Diameter ranging from 40 to 70 µm (mean= 57 µm; N=3; Fig. 4.a).

Remarks. The specimens show irregular folds on the wall which appear as darker patches and soft waves. Here we applied the criteria established by Jankauskas et al. (1989) for the classification of leiospherids. This taxon occurs as a subordinate component of the microbiota of Frecheirinha Formation.

Leiosphaeridia jacutica (Timofeev 1966) emend. Mikhaylova and Yankauskas in Jankauskas et al. 1989

Fig. 5b

1989 Leiosphaeridia jacutica Mikhaylova and Jankauskas (in Jankauskas et al. 1989): fig 3a,b,7,9

1994 Leiosphaeridia jacutica Butterfield et al.: Fig. 16H

Material. Four carbonized specimens in palynological macerations, Araticum Section (sample ARAT 29).

Description. Several thick-walled, spheroidal vesicles, characteized by a rough surface, concentric folds and diameter roughly between 100 and 200 µm. Most specimens are opaque in transmitted light, and only a few are translucent (Fig. 5b).

Remarks. The thicker walls compared to L. tenuissima cause the opaqueness of the vesicles. The species is a common constituent of Neoproterozoic microbiotas worldwide.

Genus LophosphaeridiumTimofeev (1959) , ex Downie (1963) , emend. Lister (1970)

Lophosphaeridium sp.

Fig. 5c

Material. Poorly preserved and few specimens in palynological maceration 110227/2B-2 of carbonates in the Araticum Section.

Description. Robust-walled vesicles with verrucate, plicated surface. Verrucae are less than 1 µm in diameter. Folds are prominent and the diameter of the only complete specimen observed is 46 µm. (Fig. 5.c)

Remarks. These sphaeromorphs are left in open nomenclature because of the small number of specimens observed and due to their poor preservation. Although we cannot totally rule out that these are degraded (corroded) Leiosphaeridia specimens, the regularity of the verrucae suggests that they are original structures and not taphonomic artifacts. The microfossils described under this taxon are similar to those reported by Gaucher et al. (2008) under Lophosphaeridium sp. for the Las Ventanas Formation (Uruguay).

Kingdom Eubacteria Woese and Fox (1977)

Phyllum Cyanobacteria Stanier et al. (1978)

Classis, Ordo et Fam. indet.

Genus Bavlinella (Schepeleva) Vidal (1976)

Type species. Bavlinella faveolata (Schepeleva) Vidal (1976)

Bavlinella faveolata (Schepeleva) Vidal (1976)

Fig. 6

1974 Sphaerocongregus variabilis Moorman: pls. 1-3

1976 Bavlinella faveolata Vidal : figs. 7A-C

1992 Bavlinella faveolata Schopf : pl. 54-J

2000 Bavlinella faveolata Gaucher: pl. 9, pl. 18.1-18.2

2003 Bavlinella faveolata Gaucher et al.: figs. 5C-H, 6F

2005a Bavlinella faveolata Gaucher et al.: figs. 6a-i

2006 Bavlinella faveolata Gaucher and Germs: figs. 6a-o, 7a-c

2009 Sphaerocongregus variabilis Nagy et al., figs. 1m-n

Type specimen. German et al. (1989) designated a lectotype for the species from the Kotlin Formation of the former USSR. This lectotype has also been illustrated by Schopf (1992: pl. 54-J) . Therefore, the valid designation of a lectotype supersedes any previous restriction of the application of the name of the genus and species Bavlinella faveolata. Sphaerocongregus variabilisMoorman (1974) is thus to be considered as a junior synonym (Vidal 1976, Gaucher et al. 2003).

Material. Seven specimens occur both in thin section ARAT 30 and palynological macerations (ARAT 20, 29C and 35B) of carbonates from the Frecheirinha Formation

Description. The observed specimens were mainly single spheroidal vesicles made up of tens of tightly-packed, micron-sized (1-2 μm) microspheres (Fig. 6.a), thus corresponding to the endosporangia morphotype of Moorman (1974) . Two types of preservation were observed: carbonized remains, mainly occurring in macerations, and hematized specimens (only in thin sections). Both types of preservation are common for the species (e.g. Gaucher 2000, Gaucher et al. 2003, Gaucher and Germs 2006). Diameter of vesicles ranges between 5 and 20 μm (mean=12 μm, N=17).

Remarks. B. faveolata is a subordinate component in the acritarch assemblage, which is clearly dominated by leiosphaerids. However, a few organic-rich marl layers preserve mass occurrences of B. faveolata, which is a common feature of the species (Moorman 1974, Gaucher and Germs 2006, Nagy et al. 2009).

DISCUSSION

The low-diversity fossil assemblage of the Frecheirinha Formation comprises Leiosphaeridia, Lophosphaeridium and subordinated Bavlinella faveolata (=Sphaerocongregus variabilis). Both Leiosphaeridia and Bavlinella are long-ranging microfossils, but occur as an assemblage (Table I) in the Cryogenian (e.g. Knoll et al. 1981, Nagy et al. 2009, Yin and Yuan 2007) early and late Ediacaran successions, worldwide (e.g. Germs et al. 1986, Gaucher et al. 2003, 2008, Gaucher and Germs 2006, Grey et al. 2003).

The Cryogenian occurrences are usually characterized by a strong dominance of Bavlinella faveolata in almost monospecific assemblages. Examples in North America are the Mineral Fork Formation from Utah, USA (Knoll et al. 1981) and its correlative Uinta Mountain Group in the same region (Nagy and Porter 2005), and the upper Chuar Group (Nagy et al. 2009). All these units are constrained to the lower Cryogenian, between 770 Ma and 740 Ma (Table I, Nagy et al. 2009, Link and Christie-Blick 2011). Similar, Bavlinella-dominated assemblages occur just prior to the end-Cryogenian glaciation (Table I) in the Otavi Group in Namibia (Germs et al. 2009) and in the Datangpo Formation in South China (Yin and Yuan 2007). Again in these cases, Bavlinella faveolata strongly dominates the assemblages, unlike the Frecheirinha assemblage, in which Bavlinella is a subordinated component. Furthermore, vase-shaped microfossils (VSM's) and other acritarchs occur in the Cryogenian assemblages (Nagy and Porter 2005, Huntley et al. 2006, Nagy et al. 2009), such as Cerebrosphaera, Valeria and Trachysphaeridium, none of which occur in the Frecheirinha Formation.

The evolution of acritarchs in the Ediacaran (ca. 635-541 Ma) can be divided into three phases (Gaucher and Sprechmann 2009, and references therein):

The Ediacaran Leiosphere Palynoflora (ELP; Grey 2005), re-named as Early Ediacaran Leiosphere Palynoflora (EELP: Gaucher and Sprechmann 2009), which is characterized by Leiosphaeridia-dominated assemblages, typically with large acritarchs >200 μm in diameter, and with abundance of the thick-walled Leiosphaeridia crassa (Grey 2005). Bavlinella faveolata -if present at all- is a subordinated component and acanthomorphs are absent. This assemblage occurs in successions deposited after the end-Cryogenian glacial event (635 Ma), and before the Gaskiers glacial event at ca. 580 Ma (Liu et al. 2013).

The Ediacaran Complex Acanthomorph Palynoflora (ECAP: Grey et al. 2003, Grey 2005), best represented in China and Australia (Zang and Walter 1992), but also known from other sections (e.g. Sergeev et al. 2011, Moczydlowska and Konstantin 2012) is made up of a diverse assemblage of spiny acritarchs (acanthomorphs). It has been recently divided into a lower Tianzhushania spinosa-assemblage, only represented in the lower Doushantuo Formation, and an upper, more widespread Tanarium anozos-Tanarium conoideum assemblage (Liu et al. 2013). The stratigraphic distribution of the ECAP is narrow, possibly representing between 5 and 15 Myr (Grey 2005).

The Late Ediacaran Leiosphere Palynoflora (LELP; Gaucher and Sprechmann 2009) or Kotlin-Rovno assemblage of Vidal and Moczydlowska-Vidal (1997) , marks a late Ediacaran crisis, represented by a low-diversity assemblage, characterized mainly by thin-walled Leiosphaeridia spp., more or less abundant Bavllinela faveolata, colonial microfossils of the genus Soldadophycus and small acanthomorphs of the genus Asteridium. Soft-bodied and skeletal metazoans co-occur with the depauperate acritarch assemblage. This assemblage spans the period between ca. 575-560 Ma and the Neoproterozoic-Cambrian boundary at 541 Ma (Gaucher and Sprechmann 2009).

Two Ediacaran acritarch assemblages resemble the Frecheirinha microflora, namely the EELP and LELP. The abundance of thin-walled Leiosphaeridia spp., less abundance of Bavlinella and complete absence of ECAP acanthomorphic acritarchs suggest an assignment of our fossil material to the Late Ediacaran Leiosphere Palynoflora (LELP). On the other hand, there are similarities with the Early Ediacaran Leiosphere Palynoflora (EELP). However, the absence of Leiosphaeridia crassa, the main taxon of the EELP (Grey 2005), and the common occurrence of Bavlinella militate against an assignment of the Frecheirinha microflora to the EELP. The closest counterparts of the Frecheirinha acritarchs are assemblages from (Table I) the Corumbá Group in the southern Paraguay Belt, Brazil (Gaucher et al. 2003), the Arroyo del Soldado Group in Uruguay (Gaucher 2000, Gaucher and Poiré 2009) and the Nama Group in southern Africa (Germs et al. 1986), all of which are younger than 565 Ma. They represent impoverished acritarch assemblages dominated by thin-walled Leiosphaeridia with occurrence of Bavlinella faveolata. Furthermore, all the mentioned units share similar C and Sr isotope composition of carbonates with the Frecheirinha Formation (Table I).

The apparent absence in the Ubajara Group of clear glacial deposits and sedimentary features typical of post-glacial cap carbonates (Hoffman and Schrag 2002) do not allow us to relate the Frecheirinha Formation to any glacial event, which fits a late Ediacaran age. Sedimentological evidence of such an event is so far lacking. Chemostratigraphic studies of the carbonates (Sial et al. 2003, Chiglino 2013) reported negative δ¹³C values (-3.5 ‰) at the base of the unit that may be related to periods of low plankton bioproductivity or sea level fluctuations (Gaucher et al. 2004a, Frei et al. 2011). The dark gray to black, laminated limestones of the Araticum section, start with a negative δ¹³C excursion (-3 ‰), followed by positive values up to +3 ‰ for the rest of the unit, and the samples analyzed in this study come from the interval with positive δ¹³C values.

CONCLUSIONS

The low-diversity microflora comprising Leiosphaeridia, Lophospheridium and subordinated Bavlinella, found in carbonates of the Frecheirinha Formation, is here assigned to the Late Ediacaran Leiosphere Palynoflora (LELP), and suggests a depositional age between ca. 575 and 541 Ma. These are the first Precambrian acritarchs, reported so far, from northeastern Brazil. Their thermal alteration index (TAI) between 4+ and 5, suggests metamorphic temperatures exceeding 200-250°C. Even higher temperatures, recorded at the Angustura section, are probably related to contact metamorphism of the nearby Mucambo pluton. δ¹³C values of carbonates of -3.5 ‰ VPDB at the base, passing up section into a positive plateau of up to +3.7 ‰, and ⁸⁷Sr/⁸⁶Sr values between 0.7075 and 0.7080 (Chiglino 2013) are in broad agreement with a late Ediacaran age for the Frecheirinha Formation. Given the intruding Meruoca Granite that yielded an U-Pb SHRIMP age of 541 ± 5 Ma (Santos et al. 2013) and the reported occurrence of macrofossils of the Ediacara Fauna in the overlying Jaibaras Group (Barroso et al. 2014), the depositional age of the Frecheirinha Formation may be further constrained to between 575-555 Ma. A more comprehensive palynological study of the Frecheirinha Formation is necessary to confirm this age assignment.

ACKNOWLEDGMENTS

We thank Gilsa M. Santana and Vilma S. Bezerra for their assistance with stable isotope analyses in the Laboratório de Isótopos Estaveis (LABISE). This study was partially supported by grants provided to ANS by Conselho Nacional de Desenvolvi mento Científico e Tecnológico (CNPq); CNPq - 470399/2008, CNPq 472842/2010-2, and Fundação de Amparo à Ciência e Tecnologia do Estado de Pernambuco (FACEPE) APQ 0727-1.07/08. The comments of anonymous reviewers helped improve an earlier version of the manuscript.

REFERENCES

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Publication Dates

Publication in this collection
Apr-Jun 2015

History

Received
29 Aug 2014
Accepted
19 Jan 2015

This is an open-access article distributed under the terms of the Creative Commons Attribution License

[1] BARROSO FRG, VIANA MSS, LIMA FILHO MF AND AGOSTINHO SMO. 2014. First Ediacaran Fauna Occurrence in Northeastern Brazil (Jaibaras Basin, ?Ediacaran-Cambrian): Preliminary Results and Regional Correlation. An Acad Bras Cienc 86: 1029-1042.

[2] BEURLEN K AND SOMMER FW. 1957. Observações estratigráficas e paleontológicas sôbre o calcário Corumbá. Bol Divisão Geol e Mineral/ DNPM 168: 1-47.

[3] BLANCO G, RAJESH HM, GAUCHER C, GERMS GJB AND CHEMALE JR F. 2009. Provenance of the Arroyo del Soldado Group (Ediacaran to Cambrian, Uruguay): Implications for the paleogeographic evolution of southwestern Gondwana. Precambrian Res 171: 57-73.

[4] BOGGIANI PC, GAUCHER C, SIAL AN, BAbINSKI M, SIMON CM, RICCOMINI C, FERREIRA VP AND FAIRCHILD TR. 2010. Chemostratigraphy of the Tamengo Formation (Corumbá Group, Brazil): a contribution to the calibration of the Ediacaran carbon-isotope curve. Precambrian Res 182: 382-401.

[5] BUTTERFIELD NJ AND CHANDLER FW. 1992. Palaeoenvi ronmental distribution of Proterozoic microfossils, with an example from the Agu Bay Formation, Baffin Island. Palaeontology 35: 943-957.

[6] BUTTERFIELD NJ, KNOLL AH AND SWETT K. 1994. Paleobiology of the Neoproterozoic Svanbergfjellet Formation, Spitsbergen. Fossils & Strata 34: 1-84.

[7] CAby R, SIAL AN, ARTHAUD M AND VAUCHEZ A. 1991. Crustal evolution and the Brasiliano orogeny, northeast Brazil. In: Dallmeyer RD and Lécorché JP (Eds), The West African orogens and circum-Atlantic correlative, Springer-Verlag, p. 373-397.

[8] CHIGLINO L. 2013. Quimiestratigrafía e Biostratigrafía da Formação Frecheirinha (Grupo Ubajara)-Nordeste do Brasil. PhD Thesis, Universidade Federal de Pernambuco, UFPE/BCTG 2013/320, p. 1-101.

[9] COSTA JM, DE FRANÇA JB, CAVALCANTE LINS CA, BACCHIEGGA IF, HAbEKOST CR AND BARbOSA DA CRUZ W. 1979. Geología da Bacia Jibaras Ceará, Piauí e Maranhão. Projeto Jaibaras. Ministério das Minas e Energías. DNPM. Série Geología N°14, Seção Geología Básica Nº11, p. 106.

[10] DOWNIE C. 1963. Hystrichospheres" (acritarchs) and spores of the Wenlock Shales (Silurian) of Wenlock, England. Palaeontology 6(4): 625-652.

[11] DOWNIE C AND SARJEANT WAS. 1963. On the interpretation of some hystrichosphere genera. Palaeontology 6: 83-96.

[12] EISENACK A. 1958. Tasmanites Newton 1875 und Leiosphaeridia n.g. als Gattungen der Hystrichosphaeridia. Paleontographica, Abteilung A 110: 1-19.

[13] EVITT WR. 1963. A discussion and proposals concerning fossil dinoflagellates, hystrichospheres, and acritarchs, I. PNAS 49: 158-164.

[14] FAIRCHILD TR, SANCHEZ EAM, PACHECO MLAF and LEME JM. 2012. Evolution of Precambrian Life in the Brazilian Geologial Record. Intl J Astrobiology 11: 309-323.

[15] FEDONKIN MA, SIMONETTA A AND IVANTSOV AY. 2007. New data on Kimberella, the Vendian mollusc-like organism (White Sea region, Russia): palaeoecological and evolutionary implications. In: Vickers-Rich P and Komarower P (Eds), The Rise and Fall of the Ediacara Biota. Geol Soc London Spec Publ 286: 157-179.

[16] FETTER AH, SANTOS TJS, VAN SCHMUS WR, HACKSPACHER PC, BRITO NEVES BB, ARTHAUD MH, NOGUEIRA NETO JA AND WERNICK E. 2003. Evidence for neoproterozoic continental arc magmatism in the Santa Quitéria Batholith of Ceará State, NW Borborema Province, NE Brazil: implications for the assembly of West Gondwana. Gondwana Res 6: 265-273.

[17] FREI R, GAUCHER C, DøSSING LN AND SIAL AN. 2011. Chromium isotopes in carbonates a tracer for climate change and for reconstructing the redox state of ancient seawater. Earth Plan Sci Letters 236: 28-40.

[18] FREI R, GAUCHER C, POULTON SW AND CANFIELD DE. 2009. Fluctuations in Precambrian atmospheric oxygenation recorded by chromium isotopes. Nature 461: 250-254.

[19] GAUCHER C. 2000. Sedimentology, palaeontology and stratigraphy of the Arroyo del Soldado Group (Vendian to Cambrian, Uruguay). Beringeria 26: 1-120.

[20] GAUCHER C, BLANCO G, CHIGLINO L, POIRÉ DG AND GERMS GJB. 2008. Acritarchs of Las Ventanas Formation (Ediacaran, Uruguay): implications for the timing of coeval rifting and glacial events in western Gondwana. Gondwana Res 13: 488-501.

[21] GAUCHER C, BOGGIANI PC, SPRECHMANN P, SIAL AN AND FAIRCHILD TR. 2003. Integrated correlationof the Vendian to Cambrian Arroyo del Soldado and Corumba Groups (Uruguay and Brazil) palaeogeographic, palaeoclimatic and palaeobiologic impli- cations. Precambrian Res 120: 241-278.

[22] GAUCHER C, CHIGLINO L AND PECOITS E. 2004b. Southernmost exposures of the Arroyo del Soldado Group (Vendian to Cambrian, Uruguay): palaeogeographic implications for the amalgamation of W-Gondwana. Gondwana Res 7(3): 701-714.

[23] GAUCHER C, FRIMMEL HE AND GERMS GJB. 2005a. Organic-walled microfossils and biostratigraphy of the upper Port Nolloth Group (Namibia): implications for the latest Neoproterozoic glaciations. Geol Mag 142(5): 1-21.

[24] GAUCHER C AND GERMS GJB. 2006. Recent advances in South African Neoproterozoic-Early Palaeozoic biostratigraphy: correlation of the Cango Caves and Gamtoos Groups, and acritarchs of the Sardinia Bay Formation, Saldania Belt. S Afr J Geol 109: 193-214.

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Unit	Absolute ages (Ma)	δ ¹³ Ccarb ‰V-PDB	⁸⁷ Sr/ ⁸⁶ Sr	Thin-walled Leiosphaeridia	Thick-walled Leiosphaeridia	Bavlinella	Remarks
Frecheirinha Fm.1	>560 Ma	-3.5 to +3.7	0.7075-0.7080	Dominant	Present	Subordinate
Lower Nama Group2	549-543	-4 to +5	0.7085	Dominant	Common	Subordinate	Cloudina
Lower Arroyo del Soldado Group3	<566, >532	-4.5 to +5.5	0.7070-0.7085	Dominant to common	0	Dominant to common	Cloudina
Corumbá Group4	>543	-4.5 to +5.5	0.7084-0.7086	Subordinate	0	Dominant	Cloudina
Las Ventanas Formation5	590-573	-------	--------	Dominant	0	0
Lower Pertatataka Formation6	<657 Ma	-3 to +2.5	0.7075-0.7080	Common	Dominant	0
Datangpo Formation7	663-654	--------	--------	Subordinate	Common	Dominant
Auros Fm., Otavi Group8	746-636	-6 to +8	0.7072	Present	0	Dominant
Upper Chuar Group9	>742	--------	--------	Common	Present	Dominant	Valeria lophostriata, Cerebrosphaera buickii