REVIEW ARTICLE

The Tandilia System of Argentina as a southern extension
of the Rı́o de la Plata craton: an overview

Carlos A. Cingolani

Received: 13 March 2010 / Accepted: 11 October 2010

� Springer-Verlag 2010

Abstract The southernmost outcrops of the Rı́o de la Plata

cratonic region are exposed in the Tandilia System in eastern

Argentina. The geological evolution comprises mainly an

igneous-metamorphic Paleoproterozoic basement named

Buenos Aires Complex, which is covered by Neoproterozoic

to Early Paleozoic sedimentary units which display sub-

horizontal bedding. The basement of calc-alkaline signature

consists mainly of granitic-tonalitic gneisses, migmatites,

amphibolites, some ultramafic rocks, and granitoid plutons.

Subordinate rock-types include schists, marbles, and dykes

of acid and mafic composition. Tandilia was recognized as an

important shear belt district with mylonite rocks derived

mainly from granitoids. The tectonic scenario seems related

to juvenile accretion event (2.25–2.12 Ga) along an active

continental margin, followed by continental collision

(2.1–2.08 Ga) after U–Pb zircon data. The collisional tec-

tonic setting caused thrusting and transcurrent faulting

favouring the anatexis of the crustal rocks. The tholeiitic

dykes constrain the time of crustal extension associated with

the last stages of the belt evolution. The basement was pre-

served from younger orogenies such as those of the Brasili-

ano cycle. After a long paleoweathering process, the Sierras

Bayas Group (c. 185 m thick) represents a record of the first

Neoproterozoic sedimentary unit (siliciclastic, dolostones,

shales, limestones), superposed by Cerro Negro Formation

(c. 150–400 m thick, siliciclastics) assigned to Upper Neo-

proterozoic age. The final sedimentary transgression during

Early Paleozoic was the Balcarce Formation (c. 90–450 m

thick) deposited over all the mentioned Precambrian units.

Based on all the geological background, a tectonic evolution

is offered.

Keywords Rı́o de la Plata craton � Argentina � Igneous-

metamorphic complex � Paleoproterozoic � Neoproterozoic-

Early Paleozoic cover � Tectonic model

Introduction

The Rı́o de la Plata craton is one of the continental blocks

placed at the core of western Gondwana (Almeida et al.

1973, 1976, 2000; Cordani et al. 2003). The southernmost

outcrops of this cratonic region are exposed in the Tandilia

System also called ‘Sierras Septentrionales de Buenos

Aires’ in eastern Argentina (36� 300- 38� 100 S—57�
300- 61� W). These are distributed in a 350-km-long and

maximum 60-km-wide northwest-trending orographic belt,

located in the central part of the Buenos Aires province

(Fig. 1). Marine geophysical studies show also the con-

tinuation of the belt toward the continental oceanic plat-

form. The Tandilia belt outcrops are located in between the

Salado (filled by Meso-Cenozoic units) and the Claromecó

(filled by Neoproterozoic to Paleozoic units) basins known

by exploration boreholes (Ramos 1999; Lesta and Sylwan

2005). In geomorphologic aspects, the Tandilia System is

characterized by small hills and ranges that stand out

50–250 m over the ‘pampa plain’ generally covered by

modern sediments. The Albión Hill with c. 500 m near

Tandil city is one of the highest elevations.

The geological evolution of Tandilia System comprises

mainly an igneous-metamorphic Paleoproterozoic base-

ment named Buenos Aires Complex, which is covered by

C. A. Cingolani (&)

Centro de Investigaciones Geológicas (CONICET-UNLP)

and División Cientı́fica de Geologı́a Museo de La Plata,

Calle 1 n. 644, 1900 La Plata, Argentina

e-mail: carloscingolani@yahoo.com;

ccingola@cig.museo.unlp.edu.ar

123

Int J Earth Sci (Geol Rundsch)

DOI 10.1007/s00531-010-0611-5



thin Neoproterozoic to Lower Paleozoic sedimentary

units which display sub-horizontal bedding (Teruggi and

Kilmurray 1980; Iñiguez Rodrı́guez 1999; Ramos 1999;

Cingolani and Dalla Salda 2000 and references therein). As

a final event, restricted mafic dykes intrude the sedimentary

units.

Paleomagnetic studies have been carried out in Neo-

proterozoic units of Olavarrı́a and Barker areas. The first

data was published by Valencio et al. (1980). Then studies

by Rapalini (2006) and Rapalini et al. (2008a, b) on some

samples from the Neoproterozoic cover have been per-

mitted to obtain virtual geomagnetic poles and compared

with Uruguayan localities within the Rı́o de la Plata craton

and some Gondwanan blocks. The obtained polar wander

path suggests that the Rı́o de la Plata craton during the

Neoproterozoic was localized in intermedian to low lati-

tudes and has been part of Gondwana since 570 Ma.

The Tandilia region constitutes one of the most relevant

argentine mining districts (limestones, dolostones, grani-

toids and several types of clays, among others). For this

reason, the permanent quarry activities since the XIX

century have facilitated the geological research.

Another point of view is that the Tandilia System could

be considered a ‘geopark’ because it preserved the most

ancient rocks of Argentina and Neoproterozoic primitive

microorganisms as well as the fossil structures left by them.

Many places in Tandilia are true ‘natural monuments’ that

should be preserved as geological world heritage (Cingo-

lani 2008).

The main objective of this paper is to present an update

review of the basement and its sedimentary cover of the

Tandilia System and to offer a tectonic evolution based in

the geological background.

The Tandilia System

The Tandilia geological evolution is relatively well known.

Many authors have contributed to the knowledge of the

Tandilia basement, sedimentary succession and dynamic

events since the pioneering works by Darwin (1846),

D’Orbigny (1847), Heusser and Claraz (1863), Aguirre

(1879), Backlund (1913), Nágera (1940), González Bon-

orino (1954). Basement tectonics and general stratigraphic

reviews have been provided by Teruggi and Kilmurray

(1975, 1980), Dalla Salda et al. (1988), Teruggi et al.

(1988), Dalla Salda (1999), Iñiguez Rodrı́guez (1999),

Cingolani and Dalla Salda (2000). After the first recogni-

tions of the sedimentary cover called ‘La Tinta Sandsteine’

(Heusser and Claraz 1863) or ‘La Tinta Formation’

(Nágera 1940; González Bonorino 1954) or ‘La Tinta

Group’ (Amos et al. 1972), the most widely accepted

stratigraphic scheme for the Neoproterozoic units was

proposed by Dalla Salda and Iñiguez Rodrı́guez (1979) and

subsequently modified by Poiré (1987, 1993), Iñiguez et al.

(1989); Iñiguez Rodriguez (1999 and references therein).

However, Leveratto and Marchese (1983) argued in favor

of maintaining for the Tandilia sedimentary cover, the

original name of La Tinta Formation deposited as a unique

sequence with lateral changes of lithofacies. Several geo-

logical aspects as stratigraphy, facies, lithotypes, paleon-

tology, ichnology were investigated and recorded in

publications by Borrello (1966), Teruggi and Kilmurray

(1980), Iñiguez Rodrı́guez (1999), Dalla Salda et al. (1988,

2005, 2006) and Poiré and Spalletti (2005). Mineralogical,

geochemical, sedimentary provenance and diagenetic-

hydrothermal studies were developed on several outcrops

of Tandilia (Dristas and Frisicale 1984; Dristas et al. 2003;

Zimmermann et al. 2005; Dristas and Martı́nez 2007;

Gómez Peral et al. 2007; Gaucher et al. 2008; Zimmer-

mann and Spalletti 2009).

Some review works on different aspects of Tandilia

System were published by Cingolani and Dalla Salda

(2000), Andreis (2003), Pankhurst et al. (2003), Rapela

et al. (2007), Poiré and Spalletti (2005), Dalla Salda et al.

(2005, 2006), Poiré and Gaucher (2009), Gaucher et al.

(2009), Bossi and Cingolani (2009).

Fig. 1 Location map of the Tandilia System in the Rı́o de la Plata

craton of eastern Argentina, showing the extension in between the

Salado and Claromecó basins. In red color the main outcrops of the

Paleoproterozoic rocks in Tandilia, Martin Garcı́a Island and Piedra

Alta Terrane in Uruguay. The profile shows the regional geological

relationships (after Ramos 1999). The inset maps show in the pre-drift

configuration a South America and Africa (Western Gondwana), the

location of the Rı́o de la Plata craton amalgamated with Brasiliano

belts and the relative position of the Tandilia System in South

America

Int J Earth Sci (Geol Rundsch)

123



The Paleoproterozoic basement

The igneous-metamorphic Buenos Aires Complex (Mar-

chese and Di Paola 1975a, b; Teruggi and Kilmurray 1980;

Dalla Salda et al. 1988; Cingolani and Dalla Salda 2000;

Dalla Salda et al. 2006 and references therein) assigned to

‘Transamazonian’ or Paleoproterozoic age (Fig. 2) consists

mainly of granitic-tonalitic gneisses, migmatites, amphib-

olites, some ultramafic rocks, and granitoid plutons. Sub-

ordinate rock-types include schists, marbles, and dykes of

acid and mafic composition. Conspicuous features are wide

belts of mylonites mentioned for a first time by Backlund

(1913). Metavolcanic units within the Buenos Aires

Complex have been described by Lema and Cucchi (1981,

1985) and also by Dristas (1983).

Another aspect to mention is following Teruggi et al.

(1988), the presence of a low-grade metamorphic rocks

differentiated as El Cortijo Formation and exposed only in

Tandil region, consisting of metacherts, metagreywackes

and metabasites that could represent a slice of oceanic

crust.

The igneous-metamorphic complex is partially covered

by two marine platform sedimentary units: the oldest was

described as of Neoproterozoic age, and the youngest was

assigned to an Ordovician–Silurian age. However, the

Punta Mogotes borehole near the city of Mar del Plata

revealed more than 80 m of slightly deformed metapelites

beneath the c. 400-m-thick quartz-arenites (Borrello 1962;

Di Paola and Marchese 1974; Marchese and Di Paola

1975b). According to Cingolani and Bonhomme (1982),

the metamorphic event was dated by K–Ar in illitic fine

fractions at around 600 Ma, and these metapelites are the

only rock-types that could be correlated with the Brasiliano

cycle (Ramos, 1988) in the eastern Uruguay (Cuchilla

Dionisio Belt). The Rocha Formation that outcrops in this

belt shows a similar detrital zircon pattern than that of the

Punta Mogotes Formation according to a recent study by

Rapela et al. (2008).

Regional geophysical data (gravity and magnetism)

allowed to evaluate the geometry, depth, and composition

of the Tandilia continental crust (Kostadinoff 1995), which

reaches a thickness of about 40 km. The positive gravity

Bouguer anomalies registered in this region would indicate

a slight thinning of the crust and a series of regional

alignments. Also it is possible to interpret the boundaries of

tectonic blocks associated with post-deformation main

tectonism. The record of gravity anomalies in the Balcarce-

Mar del Plata region is in accord with the presence of a c.

500-m-thick sedimentary sequence in Punta Mogotes

borehole (Kostadinoff 1995; Dalla Salda et al. 2006).

After the first geochronological data by Hart et al.

(1965), it is well known that in general the basement rocks

of Tandilia were assigned to the ‘Transamazonian’ age/

cycle (Almeida et al. 1973). It has been very common the

usage of the mentioned term (Hurley et al. 1967) as event,

cycle or orogeny to cluster all the geological processes

during the Paleoproterozoic (2000 ± 400 Ma). On the

other hand, in the local nomenclature, it was also proposed

as the ‘Tandiliano cycle’ (Ramos 1999 and references

therein). Brito Neves (2009) discussed and proposed to

Fig. 2 Geological map of the

Tandilia System showing the

main outcrop distributions of

the Paleoproterozoic crystalline

basement (Buenos Aires

Complex) and the

Neoproterozoic-Lower

Paleozoic sedimentary units

(Iñiguez et al. 1989). Note the

position of the Punta Mogotes

borehole at the Atlantic border.

Two main areas (Tandil and

Barker) were selected to show

more detailed maps

Int J Earth Sci (Geol Rundsch)

123



abandon the Transamazonian term and to use the four

Periods suggested by the International Stratigraphic Chart

published by IUGS-UNESCO on 2004 for the Paleopro-

terozoic: Siderian (2.5–2.3 Ga), Rhyacian (2.3–2.05 Ga),

Orosirian (2.05–1.8 Ga) and Statherian (1.8–1.6 Ga). In

this overview paper, we intend to use this terminology in

the interpreted tectonic model for the Tandilia System

evolution.

Metamorphic rocks

Metamorphic rocks are conspicuous in the southern and

south-eastern third of the Balcarce area. These are gneissic

rocks related to granulite facies (Fig. 3) with orthopyroxene

and hornblende; schists (El Quebracho Hill); olivine mar-

bles (Punta Tota, Bachicha Hill); pyroxene-rich ultramafic

rocks (Cinco Cerros and Punta Tota); and migmatites.

Detailed studies carried out in the El Cristo Hill near the

town of Balcarce (Dalla Salda 1975, 1999; Cortelezzi et al.

1999; Ribot et al. 2000) showed that the main metamorphic

event reached the garnet grade of the amphibolite facies that

locally underwent retrograde metamorphism.

Although non-granitic rocks are rare in the Tandil area,

there occur acid metavolcanic rocks, locally with por-

phyroblasts and comparable to rocks observed at the Vela

and at La Ribulia Hills to the South of the city of Tandil

(Fig. 4). A wollastonitic skarn has been described in the

San Miguel area. Amphibolites are observed in the Tandil

area, especially in the southern and central regions. Gran-

ulites and charno-enderbites have been found in the Azul

and Olavarrı́a areas to the NW of the System (Dalla Salda

et al. 1988, 2005; Hartmann et al. 2002b).

The metamorphic evolution of dolomitic marbles and

associated calc-silicate rocks from the interesting Punta Tota

outcrop (Balcarce region) has been reevaluated by Delpino

and Dristas (2008) through petrographic, geothermobaro-

metric, and fluid inclusion studies. These authors described

garnet migmatites showing a great abundance of pegmatitic

segregates, overlain by biotite—garnet gneisses. Metamor-

phic conditions are estimated at 750–800�C and 5–6 kb,

followed by near isobaric cooling to about 500–450�C and

5.5–6.5 kb. The studied metamorphic reactions indicate a

petrological evolution along a counterclockwise P–T path.

These authors have proposed two probable geotectonic

settings: thinning of the crust and overlying supracrustal

basin in an ensialic intraplate tectonic setting and develop-

ment of a marginal back-arc basin.

Granitoids

The above-mentioned metamorphic rocks have been intru-

ded by several granite plutons. These are typically gray

granitoids (with amazonite K-feldspars), except in the

northernmost part of the complex where the granitoid rocks

are reddish as can be observed in the Sierra Chica and other

quarries near Olavarrı́a city. In the central region of the

Complex (Tandil area) occurs a wide belt (Fig. 4) consisting

of tonalites, granodiorites, granites (partially mylonitized),

with magmatic arc affinities, possibly representing syn

to post-tectonic phases of the Paleoproterozoic (‘Trans-

amazonian’) orogeny (Dalla Salda et al. 1987, 1988). The

Alta de Vela and Montecristo leucogranites were related to

the final phase of the main orogenic event. Furthermore, the

presence of epidote-rich granite suggests a thickening and/or

a crust that was in rapid vertical motion uplift. Geochemical

tectonic discrimination analysis revealed some S-type

granite bodies (Dalla Salda et al. 1988, 2006), and the

analysis of the texture presence of feldspars, micas, and

epidote suggests a protracted thermal evolution.

Calc-alkaline and mafic—tholeiitic dyke swarm

The Buenos Aires Complex has a widespread unmeta-

morphosed dyke swarm described by Quartino and Villar

Fabre (1967), Teruggi et al. (1974b), Lema and Cucchi

Fig. 3 a Othopyroxene rich gneisses exposed at El Cristo Hill

(Balcarce area); the migmatic lensoids (white color) are evident.

b Photomicrograph of the mentioned rock showing Opx orthopyrox-

ene, Pl plagioclase, Am amphibole, Qtz Quartz, Ap Apatite, Chl
Chlorite and Op opaque mineral (courtesy of A. Ribot)

Int J Earth Sci (Geol Rundsch)

123



(1981, 1985), Dristas (1983) and Kilmurray et al. (1985).

The study of these dykes is important for an understanding

of source mantle characteristics in the Paleoproterozoic

times, as well as for insights of the processes for craton

stabilization. The oldest dykes known in Tandilia (Fig. 4)

are calc-alkaline with a bimodal composition and of

Paleoproterozoic age (Fernández and Echeveste 1995;

Iacumin et al. 1999, 2001; Teixeira et al. 2002), integrated

by andesitic to rhyolitic compositions with mainly an east–

west orientation. These calc-alkaline dykes have developed

with a thickness of 0.5–10 m and depict gray colors and

have a 40Ar/39Ar plateau age of emplacement of 2020 and

2007 Ma, contemporaneous with post-collisional intrusions

(Varela et al. 1988; Dalla Salda et al. 1992; Hartmann et al.

2002b). They originated during a transtensional stage of the

Paleoproterozoic orogeny. The calc-alkaline character has

been interpreted as representing a magmatic arc tectonic

setting (Teixeira et al. 2002). Youngest dykes from c.

1600 Ma have mafic and tholeiitic signature (Echeveste

and Fernández 1994; Iacumin et al. 2001) separated in two

sub-groups, dolerites or low-TiO2 dykes (Teruggi et al.

1974b) that outcrop in Azul and Tandil regions and high-

TiO2 basaltic dykes recorded in Tandil area (Teruggi et al.

1988). Dolerite dykes have a wide geographic distribution

(Fernández et al. 2001) as a subvertical bodies up to 50 m

thick (trending N 30� W), some with more than 5 km long.

The high-TiO2 basalt dykes have been recognized in the

Tandileufú Hill (Fig. 4) with porphyritic texture. The

phenocrysts are plagioclase, augite, with high contents of

TiO2 (1.2–1.4% by weight) and pigeonite (Dalla Salda

et al. 2005). The tholeiitic dykes, with east–west orienta-

tion cross-cutting mylonite belts and leuco-monzogranites,

indicate a significant change in the regional stress field of

the crust, with a location shift into a final Paleoproterozoic

extensional tectonic regime accompanied by an anorogenic

igneous activity.

Mylonites and shear zones

The mylonites were derived mainly from granitoids. In

Azul region, a mylonitic belt is developed in about 40 km

east–west long and 3 km wide (Gonzalez Bonorino

et al. 1956; Frisicale 1999; Ribot 2000). Another belt was

recognized south of Tandil (Fig. 4) with outcrops 25 km

long from Albión Hill to Del Tigre Range with similar

east–west orientation with some ramifications toward the

west-northwest (Dalla Salda 1981); other exposures occur

in Alta de Vela Range (Teruggi et al. 1973). Mylonites,

proto-mylonites and fault rocks are the main litho-types.

Feldspatic and amphibolitic blastesis related to these

shear zones were also described. After Ribot (2000), the

main deformation event in granitoids of the Azul region

was in medium-grade conditions (c. 450�C) followed by

hornblende alteration (rehydratation). The Azul shear

zone was interpreted based on kinematic indicators as

dextral (Gonzalez Bonorino et al. 1956) or sinistral (Ri-

bot 2000). Nevertheless, Frisicale et al. (2001, 2005)

concluded that the mylonites were developed during

lower greenschist to amphibolite facies with scarce

asymmetric rotated porphyroclasts showing both sinistral

and dextral senses of shear. After these authors, the Azul

shear zone is probably related to the late Paleoproterozoic

orogenic cycle and may be due to NNE–SSW tectonic

convergence. Deformation temperatures from mineral

assemblages are in the range of 400–450�C, and the

pressures are more than 6 kb.

Fig. 4 Geological map for the

Tandil region (Dalla Salda et al.

1988, 2006) where the

granitoids intruded the

metamorphic rocks. Note the

main distribution of the calc-

alkaline and tholeiitic dyke

swarm and the main shear zones

(mylonites)

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123



In the Sierras de Tandil shear zone, Dalla Salda (1981)

interpreted a sinistral horizontal movement. However, at

the Albión Hill, D’Angiola et al. (1992) found dextral

kinematic indicators. Based on cross-cutting relationship,

the age of the shear zones is in between 1,600 and 2000 Ma

during a Paleoproterozoic orogeny.

Geochemical and isotopic data interpretation

Dalla Salda et al. (1988, 2006) and Pankhurst et al. (2003)

offer some geochemical data based on major and trace

elements which indicate that the basement igneous-meta-

morphic rocks are of calc-alkaline composition. Rapela

et al. (2007) present also a complete set of geochemical

data, but from rocks obtained in boreholes located outside

more than 800 km to the north-west of the Tandilia Sys-

tem. The isotopic data coupled with the geochemical

characteristics obtained by these authors indicate that these

rocks are associated with intra-oceanic subduction systems

or in primitive continental arc settings.

The geochemical available data compiled by Dalla

Salda et al. (1988, 2005, 2006) show that the granitoids are

generally metaluminous but with a tendency to peralumi-

nosity in more acid varieties. Together with the predomi-

nance of hornblende, as the main mafic phase and the

absence of peraluminous minerals, the parent magmas were

interpreted as I-Type (Pankhurst et al. 2003) that is, derived

by melting of preexisting igneous source rocks. However,

several processes and sources are involved in active mar-

gins. In the tectonic discrimination diagram of Batchelor

and Bowden (1985), the majority of samples plot in the

subgroup of pre-plate collision, destructive plate margin,

subduction regime with a trend toward subgroups of syn-

collision or anatectic melting zone and post-orogenic

granites. These processes could all be involved as part of a

sequence of events beginning in a subduction-related

environment and culminating with intense deformation and

anatexis during a subsequent collisional phase. However,

the same geochemical trend extends in the other direction

for the mafic enclaves and could equally imply a coherent

geochemical and petrogenetic process for the whole suite,

such as variable partial melting of a simple mafic (tholei-

itic) source or simple mixing between tholeiitic magma and

a uniformly evolved crust.

As were shown by Rapela et al. (2007), the juvenile

geochemical and isotopic characteristics are common in

2.0–2.2 Ga rocks in the Brazilian shield corresponding to

the Paleoproterozoic (‘Transamazonian’) orogenic cycle

(Cordani et al. 2000). Studies of the major and trace ele-

ments and Sr isotope analyses on rocks collected from the

El Cortijo Formation have given rise to the view that some

of the granitoid plutons in the Tandil area are related to a

collision type tectonic setting (Dalla Salda et al. 1987;

Ramos 1988; Varela et al. 1988; Teruggi et al. 1988). The

collision favored thrusting and transcurrent faulting which

constituted a favorable condition for the initial develop-

ment of anatexis. Furthermore, it can be suggested that the

emplacement of the granite plutons in the thick gneissic

sequence in the Tandil area was coeval with the regional

high-temperature metamorphism, mylonitization and

anatexis. Some leucogranites (Alta de Vela Hill) are het-

erogeneous with high radiogenic signature and typically

post-collisional.

The calc-alkaline dykes (Iacumin et al. 2001; Teixeira

et al. 2002) have primitive mantle-normalized trace ele-

ment patterns enriched in Rb, Ba, K, La, Ce and Nd and

significant Nb and Ti anomalies, whereas the low-TiO2

tholeiitic dykes have low incompatible element contents

and primitive normalized-incompatible element patterns

with slightly positive or negative Nb, mainly reflecting

derivation from a depleted source mantle. High-TiO2 tho-

leiitic dykes have more enriched incompatible elements-

primitive mantle patterns of an enriched source mantle.

Isotopic data and its consequent interpretation were

obtained in Tandilia System basement rocks, as described

below.

K–Ar, Ar–Ar, and Rb–Sr

The oldest K–Ar ages from Tandilia are c. 2200–2000 Ma

published by Hart et al. (1965) and Halpern et al. (1970).

Other data vary between 2000 and 1500 Ma (Linares and

Latorre 1968; Teruggi et al., 1974a, 1988), but most are

younger, often less than 1000 Ma (Hart 1966; Cazeneuve

1967; Linares and González 1990). The first Rb–Sr data for

Tandilia were presented by Halpern and Linares (1970)

who gave a calculated age of 1947 ± 44 Ma for rocks in

the Olavarria area. Granites and microgranites from the San

Miguel quarry east of Tandil gave an age of 2120 ± 10 Ma

(Halpern et al. 1970; Umpierre Urquhart and Halpern

1971). The pattern of such data has been interpreted by

Teruggi and Kilmurray (1980), Dalla Salda (1981), and

Ramos (1985) as representing a series of Precambrian

events that start with sedimentation, mafic volcanism, and

nappe formation in the 2200–2000 Ma interval; followed

by intense deformation, metamorphism, and migmatization

at times c. 1800 Ma; and then granite emplacement, fold-

ing, and low-grade events during the Neoproterozoic.

Varela et al. (1988) presented a more comprehensive study

with Rb–Sr data for several areas in the Tandilia System

and obtained ages of 2154 ± 28, 2001 ± 60, 1971 ± 398,

and 1770 ± 88 Ma. Based on this isotopic information,

Dalla Salda et al. (1988, 1992) and Cingolani and Dalla

Salda (2000) have distinguished main intrusive episodes.

Pankhurst et al. (2003) obtained new Rb–Sr whole-rock

data for granitoids and orthogneisses from the western part

Int J Earth Sci (Geol Rundsch)

123



of the Tandilia System yielding an ‘errorchron’ of

2009 ± 71 Ma.

K–Ar age of 1750 ± 50 Ma for a dolerite dyke near

Tandil was obtained by Teruggi et al. (1974b). Biotites from

hornfelses adjacent to calc-alkaline (andesite–rhyolite)

dykes southeast of Azul have yielded 40Ar–39Ar ages of

2020 ± 24 and 2007 ± 24 Ma (Teixeira et al. 2001, 2002).

Plagioclase from tholeiitic dykes indicate much younger

K–Ar and 40Ar–39Ar ages of 800–1100 Ma, which is

considered to reflect hydrothermal activity (Teixeira et al.

2002).

Sm–Nd and U–Pb

Pankhurst et al. (2003) presented for granitoid samples

from Olavarrı́a region a Sm–Nd isochron of 2140 ± 88 Ma

(initial 143Nd/144Nd: 0.50977) that could record the age of

emplacement of igneous protoliths. Sm–Nd model-ages

averaging 2620 ± 80 Ma indicate that the principal rock-

forming events were a Late Archaean. Because it is likely

that these evolved granitic rocks were derived only indi-

rectly from mantle sources, with an earlier stage of crustal

differentiation, 2600–2700 Ma is considered a maximum

possible age for the original extraction of continental crust

from the mantle.

The Sm–Nd TDM model-ages obtained by Hartmann

et al. (2002b) range between 2.7 and 2.4 Ga. The eNd

values slightly below cero (-1, 27 to -3, 30) are another

argument for a crustal source for most of the Tandilia

granitoids, but this crustal source cannot be much older

than the magmatism.

Initial eNd values of 2.3–2.4 in calc-alkaline dykes

(Iacumin et al. 2001) indicate slightly more crustal con-

tamination or prehistory than that of the granitoids analyzed

by Pankhurst et al. (2003) mostly 2.1–2.2. These dykes are

essentially contemporaneous with granite emplacement in a

transtensional stage during a restricted Paleoproterozoic

orogenic activity. An upper intercept U–Pb age on two

baddeleyites from tholeiitic dyke places the intrusion at

1588 ± 11 Ma after data obtained by Teixeira et al. (2002).

Reliable ages for gneissic and granitoids rocks have

been determined by Hartmann et al. (2002b), Cingolani

et al. (2002 and 2005) using the robust U–Pb SHRIMP

isotope methodology (Fig. 5). More than 60 zircon crystals

were analyzed for samples obtained from the Azul, Tandil

and Balcarce areas.

After Hartmann et al. (2002b) regardless of composition

and structure, the magmatic ages of all zircon samples are

Paleoproterozoic (Rhyacian) in the range of 2234–2065 Ma,

with inherited ages determined in the cores of a few zircon

crystals that suggest 2368 Ma (Siderian) to 2185 (Early

Rhyacian) for the source, with only one Neoarchean age c.

2657 Ma in a tonalite from the Tandil region. Internal

structure of zircon crystals is suggestive of metamorphic

recrystallization but the ages are entirely Paleoproterozoic.

A lack of recrystallization or new zircon (Fig. 5) growth in

the Neoproterozoic suggests that the Tandilia belt was pre-

served from younger orogenies such as those of the Brasil-

iano cycle. The main tectonic activity has been linked to the

2.25–2.12 Ga accretionary event (‘Encantadas’) and to the

2.1–2.08 collisional overprint (‘Camboriu’). This geological

evolution can be correlated with the Piedra Alta terrane

(Uruguay), where Rb–Sr, Sm–Nd and U–Pb data show a

similar signature (Cingolani et al. 1997; Preciozzi et al.

1999; Hartmann et al. 2002a; Oyhantçabal et al. 2009, 2010)

during Paleoproterozoic times.

Hf isotopes

Preliminary Hf isotope analysis (Cingolani et al. 2010c) on

zircon crystals (Fig. 6) was carried out using a laser-abla-

tion microprobe, attached to a plasma multi-collector ICP-

MS at Macquarie University, Sydney (Australia). From all

studied samples taken in Tandil and Balcarce regions

suggest that the depleted mantle model age is Neoarchean

2.65 Ga, less old than the crystallization age. Positive eHf

obtained data show also derivation from juvenile material.

An alternative interpretation could be a mixing with

juvenile (2.27 Ga?) and crustal (more than 2.65 Ga) mag-

matic components. The average of 28 Hf model-ages

(c.2.6 Ga) is almost coincident to the age of the only one

inherited zircon on granitoid sample from Tandil area,

showing strong evidence supporting the derivation from a

Neoarchean crust. The Hf isotope study confirms the Sm–

Nd data published by other authors. These results are in

agreement with precise U–Pb dating of the craton in wes-

tern Uruguay and southernmost Brazil, which also indicate

a relatively short-lived Paleoproterozoic orogeny.

The Neoproterozoic-Lower Paleozoic sedimentary

cover

After more than 800 Ma Tandilia sedimentary processes

start with an unconsolidated arkosic saprolite that records a

palaeoweathering basement surface (Poiré 1987; Dristas

et al. 2003; Zalba et al. 1993). This altered level less than

4 m thick was registered in the Olavarrı́a and Barker areas.

In the currently accepted (Fig. 7) stratigraphic scheme

(Dalla Salda and Iñiguez Rodrı́guez 1979; Manassero

1986; Iñiguez et al. 1989; Poiré and Spalletti 2005; Gómez

Peral et al. 2007; Poiré and Gaucher 2009), the Sierras

Bayas Group (c. 185 m thick) is a Neoproterozoic sedi-

mentary cover comprising—from base to top- the Villa

Mónica, Colombo Diamictite, Cerro Largo, Olavarrı́a-Las

Aguilas and Loma Negra units superposed by Cerro Negro

Formation (c. 150–400 m thick) and the final sedimentary

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123



event at the Lower Paleozoic with c. 100–400 m of the

Balcarce Formation (Iñiguez et al. 1989; Iñiguez Rodrı́guez

1999; Poiré et al. 2003; Poiré 2004; Gómez Peral et al.

2007). Depositional sequences currently recognized (And-

reis and Zalba 1998; Poiré et al. 2003; Poiré and Spalletti

2005) and provenance studies (Zimmermann et al. 2005;

Zimmermann and Spalletti 2009) could be synthesized as

follow.

The first marine transgression (Villa Mónica Formation)

It was defined as the ‘‘Lower Quartzites’’ and ‘‘Dolo-

stones’’ (50–70 m thick) and bears some phosphate levels

and rich stromatolite assemblages (Poiré 1993) suggesting

a Tonian-Cryogenian age (c. 850 Ma). The main outcrops

are localized in the Olavarrı́a and Barker areas. The basal

member is composed of shallow-marine siliciclastic rocks

Fig. 5 a Backscattered electron

images of zircon crystals

analyzed by Hartmann et al.

(2002b). Samples A and B Punta

Tota (Balcarce area) banded

garnet granitoid. C Villa

Mónica quarry (Olavarrı́a) gray
charno-endeberbite. D Boca de

la Sierra (Azul) syenogranite.

E Villa Mónica quarry red

monzogranite. F Triunfo Hill

(Balcarce) mafic charnockite

gneiss. b U–Pb SHRIMP

concordia diagram for zircon

crystals of the Ta5 granitoid

sample from Montecristo quarry

(Tandil region). On the right
backscattered electron images

of two analyzed zircons

(Cingolani et al. 2005)

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123



(conglomerates, quartz-arenites, arkoses, diamictites and

shales), the upper member is characterized by shallow-

marine stromatolitic dolostones and shales (Poiré and

Spalletti 2005). The first record of acritarchs (Gaucher

et al. 2005a) in greenish pelites assigned to Leiosphaeridia

represents the oldest fossils reported for the Tandilia Sys-

tem (Fig. 7). The contact with the underlying palaeosols

(saprolite) is well exposed in some quarries in the Olavarrı́a

area (Poiré 1993). Gómez Peral et al. (2005) and Poiré

et al. (2005) reported hydrothermal pyrophyllite in shales

of the upper part of the siliciclastic member. The overlying

dolostone member includes stromatolites representing a

platform in an intertidal environment. Gómez Peral et al.

(2007) have obtained carbon and oxygen isotopic data,

combined with a detailed diagenetic study from dolostones

that provide a new record of chemostratigraphic variations

useful for regional and global correlations.

Rb–Sr geochronology of illitic shales within the dolo-

stones yielded an age of 793 ± 32 Ma (Cingolani and

Bonhomme 1988). Detrital zircon geochronology on three

samples (Rapela et al. 2007; Gaucher et al. 2008; Cingolani

et al. 2010a), show a unimodal population of Palaeopro-

terozoic age. This is a clear indication that sandstones from

different areas were mostly derived from the underlying

Buenos Aires Complex, which has a restricted Paleopro-

terozoic age range (Fig. 8).

Dristas et al. (2003) described minerals associated with

advanced argillic alteration deposits near Barker town, and

Zalba et al. (2010) have shown a complex history of weath-

ering and diagenesis of this unit in the La Juanita Range,

Barker area (Fig. 9). These authors also described well-

preserved microbially induced structures (biosignatures).

Above the mentioned unconformity, predominantly diam-

ictitic deposits of 8 m thick occur. This event recently was

recognized as a separate unit by Poiré and Gaucher (2007).

The second transgression (Cerro Largo Formation)

This second 40-m-thick marine transgression (Poiré 1993;

Poiré and Gaucher 2009) presents finely bedded, varicolored,

glauconitic sandstones, hetherolithic facies and cross-bed-

ded quartz-arenites (Fig. 7). The coarsening and shallow-

ing upward sequence represents the transition from subtidal

nearshore to shoreface environments. Chuaria, Synsphae-

ridium and Leiosphaeridia are the most important micro-

fossils found in this unit (Pöthe de Baldis et al. 1983;

Gaucher et al. 2005a). Simple trace fossils have been

reported from sandstones but were reinterpreted as desic-

cation cracks associated to biomats (Porada and Bourgouri

2008).

According to provenance geochronological studies

(Gaucher et al. 2008), the sandstones (Fig. 8) are charac-

terized by a dominant Palaeoproterozoic detrital zircon

population, but also important Archean to lowermost

Paleoproterozoic and Mesoproterozoic ages occur. The

presence of Archean detrital zircons in sandstones of this

section of the Sierras Bayas Group points to the Nico Pérez

Terrane (Uruguay), as a probably source of detritus, which

was closer to Tandilia than it is today (Gaucher et al. 2008),

and the absence of Neoproterozoic detrital zircons confirms

the deposition in a stable continental margin probably

opened to the east and south.

Shallow-marine deposits (Olavarrı́a and Las Aguilas units)

In the Olavarrı́a region quartz-arenites of the Cerro Largo

Formation pass transitionally into siltstones and claystones

of the so-called Olavarrı́a Formation (Andreis et al. 1996)

with a maximum thickness of 37 m. Rb–Sr ages on illitic

shales point to a Neoproterozoic age (Bonhomme and

Cingolani 1980). Paleoenvironmental interpretations sug-

gest shallow-marine deposits in a transgressive system

tract.

At the Aguilas Range in Barker area (Fig. 9), three

lithofacies occur in the homologous Las Aguilas Forma-

tion, from base to top (Zalba et al. 1988; Andreis 2003;

Poiré and Gaucher 2009): silicified calcareous breccias

with oolites and peloids; reddish to whitish claystones; and

a coarsening-upward, heterolithic sequence. Several sedi-

mentary structures (ripples, hummocky cross bedding and

Fig. 6 Plot of 176Hf/177Hf

ratios versus ages on dated

zircon crystals of samples from

Balcarce and Tandil regions

(Cingolani et al. 2010c). The

depleted mantle model age is

Neoarchean (c. 2.65 Ga)

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123



synaeresis and desiccation cracks) were described. Also in

the Barker area, the middle part of the unit comprises red

claystones with high iron content (32–70% Fe2O3) up to

9 m in thickness, which could be correlated with others late

Neoproterozoic iron deposits in SW Brazil and Uruguay

(Gaucher 2000; Gaucher et al. 2003, 2004). The strati-

graphic position of the Las Aguilas Formation below the

Loma Negra limestones were defined by Poiré and Spalletti

(2005) following as first suggested in Leveratto and Mar-

chese (1983) geological mapping (Fig. 9).

Open marine ramp and lagoons (Loma Negra Limestone).

Regression, karstic surface and new transgression (Cerro

Negro unit)

The Loma Negra Limestone unit was proposed by Borrello

(1966). It is the youngest depositional sequence of the

Sierras Bayas Group (Fig. 7) and has been mined for a

century by the cement industry. It is outcropping in quarries

localized in the Olavarrı́a and Barker areas (Fig. 9). The

Loma Negra Formation with 40–45 m thick is composed

Fig. 7 Integrated

lithostratigraphic column of the

Neoproterozoic-Early Paleozoic

Sierras Bayas Group, Cerro

Negro and Balcarce Formations

showing the main rock types

and unconformities based on

Poiré and Gaucher (2009).

Examples of microfossils

(Acritarchs) from Villa Mónica

and Cerro Negro units (scale
bars = 50 lm) and the

probable Cloudina cf.
C. riemkeae (scale bar 0.5 mm)

in thin sections of micritic

limestones of the Loma Negra

are after Gaucher et al. (2005a,

b). Photographs of stromatolites

(in dolostones of Villa Mónica

unit) and Arthrophycus
ichnogenus (Balcarce

Formation) are from the author

Int J Earth Sci (Geol Rundsch)

123



almost exclusively of reddish and black micritic limestones,

deposited by suspension fall-out in open marine ramp and

lagoonal environments. In these limestones, several diage-

netic processes were recognized by Gómez Peral et al.

(2007) and after chemostratigraphical studies the Loma

Negra Formation fits in global d13C and 87Sr/86Sr trends

(Kawashita et al. 1999) that range the Ediacaran age, which

is regionally important since it places constraint on the

continuity of Neoproterozoic basins in south-western

Gondwana.

On the top of the Loma Negra Formation a regional

unconformity occurs (Leanza and Hugo 1987; Barrio et al.

1991), which has been recently named ‘‘Barker Surface’’

(Poiré and Gaucher 2007; Poiré 2008) and correlated with

other Gondwanan sequences. This surface has been related

to a sea-level drop pointing to a marine regression that

exposed the Loma Negra shelf. In the micritic limestones

Gaucher et al. (2005a) reported the occurrence of Cloudina

cf. C. riemkeae (Fig. 7) and a probable medusoid resting

traces (Poiré et al. 2003). These entire data and the chemo-

stratigraphic signature (Kawashita et al. 1999; Gaucher et al.

2005a; Gómez Peral et al. 2007) suggest a Neoproterozoic

(Ediacaran) age for the upper section of the Sierras Bayas

Group. The correlation with the Arroyo del Soldado Group

(Nico Perez terrane, Uruguay) was described by Poiré et al.

(2003) and Gaucher et al. (2004).

In the Olavarrı́a region, Iñiguez and Zalba (1974)

described the Cerro Negro Formation as a 150 m thick unit

made up of illite-chlorite rich, green and reddish pelites

(Fig. 7). This unit unconformable overlies the Loma Negra

Formation. Meteoric dissolution of carbonates led to an

expressive karstic surface, in which residual clays and

brecciated cherts accumulated. At the base of the Cerro

Negro Formation, Leanza and Hugo (1987) described a

‘‘phosphate member’’ that suggests the infilling paleoval-

leys of a flat basin on a paleosurface of the Loma Negra

Formation during a marine regression. New quarry out-

crops and exploration boreholes suggest c. 400 m thick for

this unit (Poiré and Gaucher 2009) characterized by red-

dish, greenish or brown-olive-black claystones and het-

erolithic facies, mainly deposited in upper to lower

intertidal conditions. The upper contact with the Balcarce

Formation is not exposed covered by Quaternary deposits

but it was recognized in quarries exploration boreholes in

Barker region (Fig. 9). The Cerro Negro Formation yielded

abundant acritarchs in organic matter rich shales mainly

assigned to Leiosphaeridia and Synsphaeridium, which are

consistent with an Ediacaran age for the unit (Cingolani et al.

1991; Gaucher et al. 2005a). However, Rb–Sr radiometric

data (Bonhomme and Cingolani 1980) on illitic shales

suggest a Neoproterozoic age (c. 730 Ma).

Detrital zircon U–Pb ages obtained from samples loca-

ted at the base of the unit show similar polymodal pattern

reported for the Cerro Largo Formation (Fig. 8) but a

minor Archean zircon grains provenance is evident

(Cingolani et al. 2010a).

Deformation of the Neoproterozoic rocks and tangential

tectonic event

In general, the Tandilia Neoproterozoic sedimentary rocks

were slightly deformed and remained flat-lying (Iñiguez

et al. 1989). However, some deformation was described by

González Bonorino (1954) in the Olavarrı́a (Sierras Bayas)

region. Recently in a detailed work by Massabie and

Nestiero (2005) found two fold systems, F1 (NE) and F2

(NW) which define domes and basins pattern on Sierras

Bayas Group. Also ductile deformation locally observed

could be associated with a tectonic reactivation of the

Fig. 8 Comparative diagram of frequencies vs. ages for detrital

zircons for Villa Mónica Formation (Rapela et al. 2007; Gaucher et al.

2008; Cingolani et al. 2010a), Cerro Largo Formation (Gaucher et al.

2008); Cerro Negro Formation (Cingolani et al. 2010a); Sierra del

Volcán Diamictite (van Staden et al. 2010; Zimmermann and Spalletti

2009) and Balcarce Formation (Rapela et al. 2007)

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123



basement (Buenos Aires Complex), furnished by pre-

existing planar anisotropies of the mylonitized granitic

rocks. This folding is considered a result of tectonic

activity occurred during Late Precambrian to Lower Early

Paleozoic and predates the last marine transgression of the

Balcarce Formation.

As we mentioned earlier, the Punta Mogotes Formation

(metapelites) with K–Ar metamorphic age of c. 600 Ma

(Cingolani and Bonhomme 1982) could be correlated with

the Rocha Formation that outcrops in the Cuchilla Dionisio

terrane, Uruguay (Bossi and Gaucher 2004). The docking of

the Cuchilla Dionisio terrane occurred in the Cambrian

(Gaucher et al. 2005a) by means of tangential tectonics

represents one of the last events of Gondwanan amalgama-

tion. If this is correct, the Sierra Ballena Shear Zone

(c. 535 Ma) that separates this terrane from the Nico Perez

terrane could be extended through the Tandilia Atlantic

coast (Punta Mogotes borehole). Concomitant faulting block

systems (Kostadinoff 1995) has produced a deepening of the

Early Paleozoic siliciclastic basin toward the East.

New shallow-marine open shelf basin: lower Paleozoic

Balcarce unit with pyroclastic and glacial events

The last sedimentary cycle, represented by the Balcarce

Formation, crops out along the southern edge of Tandilia

from the Olavarrı́a area to Mar del Plata at the Atlantic

coast (Fig. 2). The thickest sections are exposed between

Balcarce and Mar del Plata. The Balcarce Formation

unconformable overlies all the Precambrian units (Fig. 7).

Its average thickness is 75–90 m, reaching c. 450 m in the

Punta Mogotes borehole near Mar del Plata. In general, this

unit is composed of quartzites, fine-grained quartzitic

conglomerates and kaolinitic shales. Locally at the base of

the sequence, some pyroclastic levels were described. One

of these levels was recorded at the Cerro del Corral area,

which was affected by hydrothermal solutions (Dristas and

Frisicale 1988, 2003, among others).

The sedimentological studies (Del Valle 1987a, b; Poiré

and Gaucher 2009 and references therein) suggest an epi-

continental, shallow-marine open shelf with sedimentary

facies developed in the nearshore and inner shelf environ-

ments of a tide-dominated and storm influenced platform.

The progradation to the south of the clinoforms reported by

Poiré et al. (2003) confirms that the margin of the Balcarce

basin was located to the north of the Tandilia region

(Teruggi, 1964; Dalla Salda and Iñiguez Rodrı́guez 1979).

The Balcarce Formation contains abundant and diverse trace

fossils of the ‘‘Cruziana ichnofacies’’ (Borrello 1966; Poiré

et al. 1984; Del Valle 1987b; Cingolani et al. 1985; Poiré and

Del Valle 1996; Spalletti and Poiré 2000; Seilacher et al.

2002). The age of the Balcarce Formation has been con-

sidered as early Palaeozoic. Trace fossils broadly constrain

the age between Ordovician and Lower Silurian. In the

ichnostratigraphic correlation work, Seilacher et al. (2002)

described from some localities between Balcarce and Mar

del Plata outcrops, the occurrence of Cruziana ancora an-

gusta, C. bonariensis, Diplichnites isp., Gyrochorte zigzag,

Arthrophycus alleghaniensis among other ichnospecies

(Fig. 7).

Rapela et al. (2007) reported U–Pb detrital zircon ages

(Fig. 8) from Los Pinos quarry sample with different

Fig. 9 Geological map of the

Barker area modified after

Leveratto and Marchese (1983).

The sedimentary unit

nominations were modified after

Poiré and Spalletti (2005)

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123



provenance pattern compared with the old sequences and

as young as 475–480 Ma (Early Ordovician) for the

Balcarce Formation, suggesting also a Late Ordovician to

Lower Silurian sedimentation age.

After the mineralogical, geochemical and detailed

provenance studies by Zimmermann and Spalletti (2009),

the Balcarce Formation comprises mainly detrital material

derived from old upper crustal material that excludes a

reworking of the older successions of the basement of the

Rı́o de la Plata craton, and includes Cambrian rift-related

granites of South Africa and the Sierra de la Ventana

(Eastern Argentina), as main suppliers of detritus. The

sources were magmatic, sedimentary, and subordinated

felsic metamorphic terranes. High concentrations of tour-

maline and Ti–rich heavy minerals, including zircon and

nearly euhedral chromite, are common. The delivery of

chromite may be associated with convergent tectonics

causing the obduction of oceanic crust during pre-Upper

Ordovician times (from El Cortijo Formation?). Trace

element geochemistry of recycled pyroclastic material,

associated with the quartz-arenites, also suggests volcanic

arc sources.

Recently, Cingolani et al. (2010b) present U–Pb zircon

ages by ID-TIMS on samples taken from kaolinitized

pyroclastic levels outcropped in Cerro del Corral (Dristas

and Frisicale 1988). The studied zircon crystals show

mainly idiomorphic bi-pyramidal type characteristics,

suggesting acidic igneous origin and reveal a very few

transport from the source. The analyzed zircons indicate

much older ages than the Ordovician–Silurian age of

Balcarce sedimentation. Most of 207Pb/206Pb ages are close

to 2.1 Ga, suggesting a main Paleoproterozoic source area

for these crystals, representing the typical age of the

Tandilia basement. Among the 18 analyzed zircon frac-

tions, extracted from volcaniclastic layers, no evidence of

an Ordovician–Silurian volcanic episode was obtained,

suggesting that these crystals represent a re-working

product of previous Paleoproterozoic volcanic rocks.

Diamictite levels were recognized at the Sierra del

Volcán, Balcarce area (Spalletti and Del Valle 1984) in

between the crystalline basement and the Balcarce For-

mation. This diamictite is 4 m thick and bears polihedrical

dropstones, often in vertical position, affecting both ripple

bedding and lamination structures. Based on its strati-

graphic position, the Sierra del Volcán Diamictite was

originally considered to represent an Ediacaran glacial

event (Spalletti and del Valle 1984; Pazos et al. 2008).

However, Poiré and Spalletti (2005) and Zimmermann and

Spalletti (2009) suggested a possible Hirnantian age for

these glacial event, as a member of the Balcarce Formation

deposits on the basis of Ordovician U–Pb ages (Fig. 8) of

detrital zircons reported by van Staden et al. (2010).

Therefore, this glacial unit should be referred to the Upper

Ordovician, which can be correlated with an important

glacial event in southern South America and South Africa.

As a final event. some subalkaline dolerite sills intrude

kaolinitic shales assigned to the Balcarce Formation in Los

Barrientos area (Rapela et al. 1974) yielded whole-rock

K–Ar ages of 450 and 490 Ma. However, at the Cerro del

Corral a dolerite sample obtained from the mining explo-

ration borehole (Cingolani et al. 1985) yielded a K–Ar

whole-rock age of 396 ± 11 Ma and it is tentatively cor-

related to the outcrops of Los Barrientos area.

Diagenetic and hydrothermal activity

In the Tandilia System, several evidence of hydrothermal

activity (clay deposits, quartz crystals, alunite and iron-rich

levels) were recognized (Dristas and Frisicale 1988; Dristas

et al. 2003). The latter described in the sedimentary cover

(Balcarce Formation), an alteration of original fall-out

pyroclastic material at Cerro del Corral area, showing a

kaolinite and rutile-anatase assemblage from low-temper-

ature process. Other deposits involving mainly reworked

pyroclastic material were located in the west of Barker,

Sierra de la Tinta areas (Fig. 9) displaying an advanced

argillic alteration, which include pyrophillite, kaolinite,

dickite, rutile, alunite, diaspore, hematite and secondary

quartz as mineral association. There are also deposits

derived from alteration of migmatites from the basement

complex rocks, showing advance argilic alteration repre-

sented by pyrophyllite, kaolinite, sericite, diaspore, hema-

tite, alunite, tourmaline, and rutile. The interpretation done

by Dristas and Frisicale (1984) was that these deposits

occur along faults, fractures and breccias through which the

hydrothermal fluids could be mobilized. The consequent

mixing hydrothermal solutions with meteoric water gave

rise to more oxidizing conditions and to the formation of

alunite veins. The iron-rich deposits of the Barker region

were studied by Dristas and Martı́nez (2007) that con-

cluded they were formed under low temperature conditions

and are related to an unconformity with a large-scale

hydrothermal activity. The source of iron may be assigned

to the alteration of mafic minerals of the migmatitic

Paleoproterozoic basement during a Late Precambrian age

(616 ± 17 Ma, K–Ar data). As was mentioned earlier,

Gómez Peral et al. (2007) have studied the diagenetic

processes, divided into several stages that affected the

dolostones from the lower part of the sedimentary cover

(Villa Mónica Formation) and the carbonaceous Loma

Negra Formation.

Stratigraphic correlations and tectonic setting

The Neoproterozoic-Early Paleozoic marine deposits,

initially known as ‘La Tinta Sandsteine’, as a Formation

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123



(or as Group) now composed of the Sierras Bayas Group,

Cerro Negro and Balcarce Formations, were correlated

with the Nama Group in southwest Africa (Germs 1972;

Dalla Salda 1979, 1980, 1982, Dalla Salda et al. 1988), that

records the assembly of southwestern Gondwana during the

Neoproterozoic. On the other hand, Aceñolaza (1978)

mentioned this correlation and described the common

Neoproterozoic-Lower Paleozoic sequences as the ‘‘Nama-

La Tinta basin’’.

More recently, Gaucher et al. (2005a) based on litho, bio

and chemostratigraphy have compared the Tandilia Neo-

proterozoic sedimentary successions with the lower section

of the Arroyo del Soldado Group (Nico Pérez terrane,

Uruguay). Both are characterized by alternation of carbo-

natic and siliciclastic members deposited in a passive

margin tectonic setting. Despite the Arroyo del Soldado is

up to 5 km thick, the Neoproterozoic of Tandilia records a

shallower epicontinental condensed section showing ero-

sive surfaces in a 350–400 m thick profile.

The isotopic signatures of Loma Negra limestones, the

possible occurrence of shelly fauna elements (Cloudina)

and a karstic surface developed on the top of the carbon-

ates, indicate main SW Gondwanan sea-level drop and

platform exposure (Poiré and Gaucher 2007; Poiré 2008).

The low diversity acritarchs assemblages in siliciclastic

units were also used for stratigraphic correlations, making a

direct connection with similar time intervals in Uruguay

and Brazil (Corumbá Group). The correlations suggested

by Gaucher et al. (2005a, b) imply that an extensive marine

shelf opened toward the East was developed on a large area

of the ‘Rı́o de la Plata paleocontinent’ during the Neo-

proterozoic. Tropical paleoclimate conditions in a tectonic

quiescence and far from Brasiliano/Pan-African orogenic

belts (Gaucher 2000, 2007; Gaucher et al. 2003, 2005a)

have been recognized.

Finally, the last transgression of the Balcarce Formation

could be correlated after Zimmermann and Spalletti (2009)

with similar rocks in the Cape Fold Belt of South Africa,

the Peninsula Formation, and the upper Table Mountain

Group (Windhoek and Nardouw Subgroups) and partially

with the lower sedimentary Sierra de la Ventana sequences.

Tectonic evolution

The evolution model could be represented by time stages

(Figs. 10, 11) using the IUGS Precambrian subdivisions as

suggested by Brito Neves (2009), as follow.

Neoarchean-Siderian (Fig. 10, stage 1)

In a first stage (c. 2.2 Ga), a juvenile evolution of sep-

arated continental blocks as suggested by petrological,

geochemical and isotopic data was developed. Based on

isotopic evidence, the protolith of the rock crust could

be Neoarchean (c. 2.5–2.6 Ga). Subduction-related mag-

matic arcs were developed (Teruggi et al. 1988). After

Ramos (1999) were interpreted the interaction with

Buenos Aires, El Cortijo and Tandilia continental blocks

related in a subduction tectonic setting. This tectonic

scenario was mentioned by Hartmann et al. (2002b) as

the ‘Encantadas Orogeny’ based on U–Pb SHRIMP

zircon data.

Early-Late Rhyacian (Fig. 10, stage 2)

At this stage was interpreted a continent–continent colli-

sional event, as suggested by the thick mylonites belts, the

presence of ocean floor rocks, and the presumed thickening

of the crust (c. 2.2–2.0 Ga). The collision caused thrusting

and transcurrent faulting favoring the anatexis of the

crustal rocks. Furthermore, the emplacement of the gran-

itoid plutons in the thick gneissic sequence in the Tandil

area could have been coeval with the regional high-tem-

perature metamorphism, mylonitization, and calc-alkaline

dykes during a transtensional event and as a consequence

anatexis processes occurred. After Hartmann et al. (2002b),

this event corresponds to the collisional ‘Camboriú

Orogeny’.

Orosirian-Statherian (Fig. 10, stage 3)

At this stage, it took place the generation of heterogeneous,

highly radiogenic and typically post-collision leucograni-

toids (c. 1.8 Ga). The dolerite dykes (c. 1.6 Ga) constrain

the time of crustal extension associated with the last stages

of Tandilia basement evolution.

Early Mesoproterozoic to Late Neoproterozoic

(Fig. 10, stages 4 and 5; Fig. 11 stage 6)

The igneous-metamorphic basement suffered a long period

of peneplanization, paleoweathering and generation of an

arkosic saprolite (c. 1.6–0.9 Ga). The Tandilia basement

was variably affected by hydrothermal overprints. During

Late Neoproterozoic developed a first marine transgres-

sion with siliciclastic and stromatolite-rich dolostones

over a highly weathered Paleoproterozoic basement.

Separated with an unconformity, a second sedimentary

transgression was developed with siliciclastic and lime-

stone units. After that a karstic surface and an iron-

phosphoric level record the regression and sea-level drop

event (Leanza and Hugo 1987; Poiré and Gaucher 2007;

Gómez Peral et al. 2007). A new marine transgression was

described as a final Neoproterozoic siliciclastic sedimen-

tary event.

Int J Earth Sci (Geol Rundsch)

123



Late Neoproterozoic-Cambrian (Fig. 11 stage 7)

A probable tangential tectonic could have developed in

relation with the docking of the Cuchilla Dionisio Ter-

rane in Uruguay. Some deformation of the Neoprotero-

zoic sedimentary units already described predates the

Early Paleozoic Balcarce Formation. Then an important

block faulting occurred as expression of a compressional

event in response to south-west stress (Iñiguez et al.

1989). Due to vertical tectonic movements, the Palaeo-

proterozoic basement was uplifted by normal faulting; the

depressed blocks preserved most of the Neoproterozoic

Fig. 10 Diagrams (orientated

NW–SE) of the interpreted

tectonic evolution by time slices

(see stages 1–5) for the Tandilia

System showing: subduction arc

setting of continental blocks

(after Teruggi et al. 1988;

Ramos 1999), main collisions,

thickening crust, transcurrent

faults, anatexis events, final

extension with dolerite dykes

and cratonization (Dalla Salda

et al. 2006). The sedimentary

cover starts with an arkosic

saprolite and first siliciclastic-

dolostone marine transgression

occurred (Iñiguez et al. 1989)

Int J Earth Sci (Geol Rundsch)

123



sedimentary cover only in Sierras Bayas and Barker

areas.

Ordovician to Silurian (Fig. 11, stage 8–80)

After the erosive stage, a new transgression developed over

the latter tectonic scenario covering all the mentioned

blocks. A diamictite member is an evidence of a Hirnantian

glacial event. Hydrothermal iron-rich levels occurred as

described by Dristas and Martı́nez (2007). It is important to

note that the thickest section of the Balcarce Formation

unconformably lying over the Punta Mogotes Formation

(c. 600 Ma K–Ar metamorphic ages) was recorded toward

the east in the Atlantic borehole.

Upper Paleozoic

Zalba et al. (2007) confirmed that after the uplift and

reactivated faulting that occurred during the Middle Perm-

ian, the Tandilia System has remained as a positive area.

Toward north the rift-related (aulacogene) Salado basin was

opened and filled Meso-Cenozoic sequences. To the south,

the Claromecó basin (and the Ventania System) was intense

deformed during Permian times (see profile of Fig. 1).

Fig. 11 Second part of the

interpreted tectonic evolution

diagrams (see stages 6–80)
showing a new marine

transgression (siliciclastic and

micritic carbonates), regression

and sea-level drop with karstic

surface developed. Inset detail

after Leanza and Hugo (1987).

Then another marine

transgression occurred

(siliciclastics). A probable

tangential tectonic could have

developed in relation with the

docking of the Cuchilla

Dionisio terrane (Uruguay).

Deformation of the

Neoproterozoic sedimentary

units predates the Balcarce

Formation. Then an important

block faulting occurred as

expression of a compressional

event in response to south-west

stress (Iñiguez et al. 1989). The

Palaeoproterozoic basement

was uplifted by normal faulting

but the depressed blocks

preserved most of the

Neoproterozoic sedimentary

cover only in the Sierras Bayas

and Barker areas. A final

Balcarce transgression occurred

over all the mentioned

Precambrian units. A diamictite

glacial event was described

(Zimmermann and Spalletti

2009) and some iron-rich

hydrothermal processes were

studied by Dristas J and

Martı́nez (2007) as we shown in

the detail inset. The last stage

shows the thickest section of the

Balcarce Formation that was

recorded toward the east in the

Atlantic Punta Mogotes

borehole (see inset)

Int J Earth Sci (Geol Rundsch)

123



Final remarks

1. The southernmost outcrops of the Rı́o de la Plata

cratonic region are well exposed in the Tandilia Sys-

tem also called ‘Sierras Septentrionales de Buenos

Aires’ in eastern Argentina.

2. The igneous-metamorphic Buenos Aires Complex

assigned to ‘Transamazonian’ or Paleoproterozoic age

consists mainly of granitic-tonalitic gneisses, migma-

tites, amphibolites, some ultramafic rocks and granitoid

plutons. Subordinate rock-types include schists, mar-

bles, and dykes of acid and mafic composition.

Conspicuous features are wide belts of mylonites.

3. The isotopic data coupled with the geochemical char-

acteristics indicate that the igneous-metamorphic base-

ment rocks are associated with intra-oceanic subduction

systems or in primitive continental arc settings.

4. After U–Pb data, a lack of recrystallization or new

zircon growth in the Neoproterozoic suggests that the

Tandilia basement was preserved from younger orog-

enies such as those of the Brasiliano cycle. This

geological evolution can be correlated with the Piedra

Alta terrane (Uruguay), where Rb–Sr, Sm–Nd and

U–Pb data show a similar signature during Paleoprote-

rozoic times. The average of Hf model-ages (c.2.6 Ga)

shows strong evidence supporting the derivation from

a Neoarchean crust that indicates a relatively short-

lived Paleoproterozoic orogeny.

5. The igneous-metamorphic complex is partially cov-

ered by two marine platform sedimentary units: the

oldest was described as of Neoproterozoic age, and the

youngest was assigned to an Ordovician–Silurian age.

In the currently accepted stratigraphic scheme the

Sierras Bayas Group (c.185 m thick) is a Neoprotero-

zoic sedimentary cover superposed by Cerro Negro

Formation (c. 150 to 400 m thick) and the final

sedimentary event at the Lower Paleozoic with c.

100–400 m of the Balcarce Formation.

6. The Tandilia sedimentary cover were slightly

deformed and remained flat-lying. However, some

deformation was described in the Olavarrı́a (Sierras

Bayas) region.

7. Several evidence of hydrothermal activity (clay depos-

its, quartz crystals, alunite and iron-rich levels) were

recognized.

8. The tectonic evolution model could be represented by

time stages starting in the Neoarchean-Siderian with

subduction arc setting of continental blocks, follow by

main collisions, thickening crust and anatexis during

Early-Late Rhyacian and continuous during Orosirian-

Statherian with the final extensional dykes and

cratonization.

9. The basement rocks suffered a long period of penepl-

anization and paleoweathering during the Mesoprote-

rozoic to Early Neoproterozoic.

Acknowledgments I would like to thank the editors S. Siegesmund

and M. Basei for their kind invitation to participate in this special

issue. This review work has been benefited by stimulating discussions

during the last years with my colleagues Luis H. Dalla Salda, Ricardo

Varela, Héctor Leanza, Daniel Poiré, Florencio Aceñolaza, Alejandro

Ribot, Vı́ctor A. Ramos, Jorge Bossi, Claudio Gaucher, Marcelo

Manassero and Eduardo Llambı́as. Thanks to Norberto Uriz for rel-

evant support for drawing the final version of some figures and many

discussions during field and laboratory works. I would like to thank

Mario Campaña and Andrea Bidone for their technical support. This

study was enabled by grants from CONICET (PIP 5027 and 0647).

The revision by Umberto Cordani, Pedro Oyhantçabal, anonymous

reviewer and the Editor S. Siegesmund helped to improve this man-

uscript and are deeply acknowledged.

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