Accepted Manuscript

Tectonomagmatic Setting And Provenance Of The Santa Marta Schists, North‐

ern Colombia: Insights On The Growth And Approach Of Cretaceous Caribbean

Oceanic Terranes To The South American Continent

A. Cardona, V. Valencia, C. Bustamante, A. García-Casco, G. Ojeda, J. Ruiz,

M. Saldarriaga, M. Weber

PII: S0895-9811(09)00142-4

DOI: 10.1016/j.jsames.2009.08.012

Reference: SAMES 862

To appear in: Journal of South American Earth Sciences

Received Date: 26 August 2008

Accepted Date: 26 August 2009

Please cite this article as: Cardona, A., Valencia, V., Bustamante, C., García-Casco, A., Ojeda, G., Ruiz, J.,

Saldarriaga, M., Weber, M., Tectonomagmatic Setting And Provenance Of The Santa Marta Schists, Northern

Colombia: Insights On The Growth And Approach Of Cretaceous Caribbean Oceanic Terranes To The South

American Continent, Journal of South American Earth Sciences (2009), doi: 10.1016/j.jsames.2009.08.012

This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers

we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and

review of the resulting proof before it is published in its final form. Please note that during the production process

errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

ACCEPTED MANUSCRIPT

TECTONOMAGMATIC SETTING AND PROVENANCE OF THE SANTA

MARTA SCHISTS, NORTHERN COLOMBIA: INSIGHTS ON THE GROWTH

AND APPROACH OF CRETACEOUS CARIBBEAN OCEANIC TERRANES TO

THE SOUTH AMERICAN CONTINENT

Cardona, A.1,2, Valencia, V.3, Bustamante, C.4, García-Casco, A.5, Ojeda, G.2, Ruiz,

J.3, Saldarriaga, M.4, Weber, M6.

1Smithsonian Tropical Research Institute, Ancón, Panama

2 Instituto Colombiano del Petróleo, Piedecuesta, Colombia

3 Department of Geosciences, University of Arizona, USA

4Departamento de Geología, Universidad EAFIT, Colombia

5Departamento de Mineralogia y Petrología, Universidad de Granada, España

6Escuela de Geociéncias y Medio Ambiente, Universidad Nacional, Medellín,

Colombia

Abstract

Metamorphosed volcano-sedimentary rocks accreted to the northern South American

continental margin are major vestiges of the Caribbean oceanic plate evolution and its

interactions with the continent. Selected whole rock geochemistry, Nd-Sr isotopes and

detrital zircon geochronology were obtained in metabasic and metasedimentary rocks from

the Santa Marta and San Lorenzo Schists in northernmost Colombia. Trace element

patterns are characterized by primitive island arc and MORB signatures. Similarly initial

87Sr/86Sr- �Nd isotopic relations correlate with oceanic arcs and MORB reservoirs,

suggesting that the protoliths were formed within a back-arc setting or at the transition

ACCEPTED MANUSCRIPT

between the inta-oceanic arc and the Caribbean oceanic crust. Trace element trends from

associated metasedimentary rocks show that the provenance was controlled by a volcanic

arc and a sialic continental domain, whereas detrital U/Pb zircons from the Santa Marta

Schists and adjacent southeastern metamorphic units show Late Cretaceous and older

Mesozoic, Late Paleozoic and Mesoproterozoic sources. Comparison with continental

inland basin suggest that this arc-basin is allocthonous to its current position, and was still

active by ca. 82 Ma. The geological features are comparable to other arc remnants found in

northeastern Colombia and the Netherland Antilles. The geochemical and U/Pb detrital

signatures from the metasedimentary rocks suggest that this tectonic domain was already in

proximity to the continental margin, in a configuration similar to the modern Antilles or the

Kermadec arc in the Pacific. The older continental detritus were derived from the ongoing

Andean uplift feeding the intra-oceanic tectonic environment. Cross-cutting relations with

granitoids and metamorphic ages suggest that metamorphism was completed by ca. 65 Ma.

Introduction

The accretion of oceanic and continental terranes is a major factor of growth and

modification of convergent margins (Howell, 1995, Sengör and Natal'in, 1996). The life

cycle of these terranes includes several phases of magmatic growth, accretion of other

terranes and translation before reaching a continental margin (Howell, 1995, Shervais,

2001). To reconstruct each of these phases is of major importance in order to understand

the tectonics and paleogeography of oceanic domains that are commonly destined to lose

their unity during subduction. The Cretaceous to Paleogene tectonic evolution of the

northern margin of South America is influenced by its interaction with the Caribbean

oceanic plate, as part of an ongoing Wilson cycle that started with the break-up of the

ACCEPTED MANUSCRIPT

Pangea Supercontinent in the Late Jurassic (Pindell, 1993, Pindell and Keenan, 2001).

Several ophiolite and mafic volcanic sequences recognized along the Northern Andes and

the Caribbean coast of Colombia, Ecuador and Venezuela (Figure 1) have shown a

complex series of oceanic-continent interactions which still are not fully understood (Kerr

et al., 1997, 2002, Giunta et al., 2002, 2003, Pindell et al., 2005, Sisson et al., 2005, Weber

et al., in press).

In fact, due to the disruption and dispersion of these complexes by the eastern displacement

of the Caribbean plate and the remobilization by younger events, accurate tectonic models

and paleogeographic reconstruction must consider integrated information from each

Circum-Caribbean region (Iturralde-Vinent and Lidiak, 2006).

In this contribution we integrate geological considerations, whole rock geochemistry, Nd

and Sr isotopes, and U/Pb detrital zircon geochronology from the metamorphosed volcano-

sedimentary Santa Marta schist belt in northern Colombia. These results are used to

reconstruct the tectonomagmatic evolution of the protoliths, define their provenance and

placed them into the current models that include major stages of translation and accretion of

the Caribbean oceanic fragments to the South American margin during the Late Cretaceous.

Geological Setting

The transition of the northern Colombian Andes to the Caribbean region is characterized by

several isolated massifs surrounded by Cenozoic basins (Figure 2). This configuration is

related to Late Meso-Cenozoic east-northeast migration of the Caribbean plate and the

escape tectonics of the northern Andean block related to the subduction of the Pacific plate

(Kellog, 1984, Colletta et al., 1997; Taboada et al., 2000, Montes et al., 2005). The Santa

Marta Massif within the northern Caribbean region of Colombia is an uplifted region that

covers an area of 13.700 Km2 with altitudes of ca. 5.900 m. This massif is formed of

ACCEPTED MANUSCRIPT

predominantly crystalline rocks and can be divided into three different belts with a well

defined outboard younging pattern (Figure 2), that shares some similarities with the main

northern Andean domains (reviews in Tschanz et al., 1974, Cordani et al., 2005, Cardona-

Molina et al., 2006). The southeasternmost belt includes ca. 1.0-1.2 Ga inliers of high grade

metamorphic rocks, that are part of the more extensive Grenvillian orogenic belt dispersed

along the Colombian Andes (reviews in Cordani et al., 2005). Jurassic plutons and

volcanites intrude and cover this metamorphic unit, whereas minor Carboniferous and Late

Mesozoic sedimentary sequences rest in unconformity towards the southeast flank (Tschanz

et al., 1969, 1974, Rabe, 1977). The intermediate belt includes an intercalation of

amphibole and mica-schists of Paleozoic age with Permian mylonitic granitoids (Tschanz et

al., 1969, Cardona-Molina et al., 2006, Cardona et al. submitted). The northwestern and

youngest belt comprises of an imbricate series of Cretaceous greenschist to amphibolite

facies metavulcano-sedimentary units with orthogneisses (Doolan, 1970, MacDonald et al.,

1971, Tschanz et al., 1974, Cardona et al., submitted). The Cesar-Rancheria basin is

exposed in the southeastern flank of the Santa Marta Massif and represents a sedimentary

record that evolved from Cretaceous passive margin to Maastrichian-Paleogene orogenic

deposits that are linked to an accretionay and subduction related event of the Caribbean

plate (Bayona et al., 2007). The geologic evolution of the Cretaceous metamorphic units

has been related to a broader belt that outcrops in northeasternmost Colombia, the

Netherland Antilles and Venezuela, and was named the Ruma belt (MacDonald et al.,

1971). Here we will place this fragment as part of an accreted Mesozoic oceanic domain

linked to the Caribbean - South America plate tectonic interaction. Paleogene granitoids

intrude the different belts sealing the accretionary events at ca. 65 Ma (Tschanz et al., 1974,

ACCEPTED MANUSCRIPT

Cardona et al., submitted). More details on the nature of this metamorphic unit that

represents the scope of this paper will be discussed in the next chapter.

Geology of the Santa Marta belt

The Santa Marta Province as defined by Tschanz et al. (1969, 1974) includes two major

metamorphic belts (Figure 2) separated by an extensive Paleogene granitoid belt (Tschanz

et al., 1974). The southeastern belt includes a series of amphibolites, two-mica schists and

orthogneisses metamorphosed in the upper-greenschist to amphibolite facies. These units

have been named the San Lorenzo, Gaira and Undifferentiated Schists (Tschanz et al.,

1969). Recent geochronological data on an orthogneiss unit from this belt have shown the

existence of a Turonian (ca. 90 Ma) arc related plutonism, whereas geological observations

on the southeastern contact with the Paleozoic rocks have shown that the continental

margin basement and its cover were probably deformed together during the Late

Maastrichian (Cardona-Molina et al., 2006, Cardona et al., 2008).

The outer coastal metamorphic rocks, which are the major objective of this paper, were

mapped in detail by Barry Doolan during the 70s, who included them in the Santa Marta

Schists (SMS). This belt was subdivided in four major units with stratigraphic connotation:

from northwest to the Concha, Punta Betín, Cinto and Rodadero Formations (Figure 3).

This subdivision is followed in this paper, and discussed in light of new observations and

sampling in the vicinity of the city of Santa Marta (Figure 3).

The principal metamorphic foliation of the belt trends to the northeast, dipping between

37°-70° to either the SE or NW. Several The northwestern Concha Formation includes an

intercalation of quartzfeldspathic schists and chlorite-actinolite schists with carbonates.

Minor coarse-grained amphibolites are also tectonically intercalated and associated to some

major fault zones. The Punta Betín unit comprises predominantly actinolite-schists and

ACCEPTED MANUSCRIPT

amphibolites with minor intercalations of muscovite-schists. Some metachert and quartzite

bodies were also described by Doolan (1970). The contact with the Concha Formation is

considered tectonic and related to the southward thrust of the Punta Betín unit (MacDonald,

1971). Metamorphic grade in both units is not dramatically different, both of them

metamorphosed in the greenschist facies. The Cinto Formation is a metasedimentary

sequence that presents stratigraphic contacts with the Punta Betín Formation. It includes

garnet bearing muscovite-schists. The southeastern Rodadero Formation is made up by

amphibolites and amphibole-schists intercalated with mica-schists. The presence of

pyroxene in the amphibolites indicates high amphibolite facies metamorphic conditions.

Available geochronological constrains from the Santa Marta belt include a series of K-Ar

amphibole, biotite and whole rock ages ranging between 33 Ma and 130 Ma (MacDonald et

al., 1971, Tschanz et al., 1974). These results seems to be related to thermal resetting and

cooling associated with the extensive Paleogene plutonism that intrudes these rocks

(MacDonald et al., 1971, Cardona et al submitted). Two of the three older ages of ca. 110-

130 Ma have very high errors probably related to low-K contents in the analyzed

amphiboles. However, there seems to be a more precise 110 ± 8.8 Ma age, but due to the

analytical limitations of the K-Ar method it is not possible to confidentially evaluate its

meaning (presence of either argon loss or excess).

We have attempted to date two samples with the Ar/Ar method in the same localities were

MacDonald et al. (1971) have done their previous K-Ar analysis. However, low-K contents

have yielded high analytical errors, although there seems a clear suggestion of Paleogene

argon loss there are also evidence of older Ar ages. Recent U-Pb zircon analysis of

metamorphic rims from a garnet-biotite coarsed grain schist of the Rodadero Formation

ACCEPTED MANUSCRIPT

have yielded ages of ca. 65 Ma which we are related to a late metamorphic event and the

post-tectonic magmatism (Cardona et al., 2009).

Analytical techniques

Geochemistry

Bulk whole rock chemical analysis of 24 samples was determined by inductively coupled

plasma-mass spectrometry (ICP-MS) at Acme Analytical Laboratories Ltd. in Vancouver,

Canada. A 0.2 g aliquot is weighed into a graphite crucible and mixed with 1.5 g of LiBO2

flux. The crucibles are placed in an oven and heated to 1050° C for 15 minutes. The molten

sample is dissolved in 5% HNO3.Calibration standards and reagent blanks are added to the

sample sequence. Sample solutions are aspirated into an ICP emission spectrograph (Jarrel

Ash Atom Comb 975) for determining major oxides and certain trace elements (Ba, Nb, Ni,

Sr, Sc, Y & Zr), while the sample solutions are aspirated into an ICP-MS (Perkins-Elmer

Elan 6000) for determination of the trace elements, including rare earth elements. Results

are presented in Tables 1 and 2.

U/Pb LAM-ICP-MS

U/Pb analyses were done at the Arizona LASERCHRON laboratoy following the

procedures described by Dickinson and Gehrels (2003) and Gehrels et al. (2008).

Results are included in Table 4. Unknowns and standard zircons were mounted in the

central half of the mount area, to reduce possible fractionation effects. The grains analyzed

were selected randomly from all of the zircons mounted from each sample. In detrital

samples core of grains were preferred to avoid possible thin metamorphic overgrowth.

Zircon crystals were analyzed in polished epoxy grain mounts with a Micromass Isoprobe

multicollector ICPMS equipped with nine Faraday collectors, an axial Daly collector, and

four ion-counting channels. The Isoprobe is equipped with an ArF Excimer laser ablation

ACCEPTED MANUSCRIPT

system, which has an emission wavelength of 193 nm. The collector configuration allows

measurement of 204Pb in the ion-counting channel while 206Pb, 207Pb, 208Pb, 232Th and 238U

were simultaneously measured with Faraday detectors. All analyses were conducted in

static mode with a laser beam diameter of 35-50 diameter, operated with an output energy

of ~32 mJ (at 23 kV) and a pulse rate of 9 Hz. Each analysis consisted of one 20-second

integration on peaks with no laser firing and twenty 1-second integrations on peaks with the

laser firing. Hg contribution to the 204Pb mass position was removed by subtracting on-peak

background values. Inter-element fractionation was monitored by analyzing an in-house

zircon standard, which has a concordant TIMS age of 564 ± 4 Ma (2�) (Gehrels,

unpublished data). This standard was analyzed once for every five unknowns in detrital

grains. Uranium and Th concentrations were monitored by analyzing a standard (NIST 610

Glass) with ~500 ppm Th and U. The lead isotopic ratios were corrected for common Pb,

using the measured 204Pb, assuming an initial Pb composition according to Stacey and

Kramers (1975) and respective uncertainties of 1.0, 0.3 and 2.0 for 206Pb/204Pb, 207Pb/204Pb,

and 208Pb/204Pb.

The age of standard, calibration correction from standard, composition of the

common Pb, and the decay constant uncertainty are grouped and are known as the

systematic error. For these samples the systematic errors range between ~1.0-1.4% for

206Pb/238U and ~0.8-1.1% for 206Pb/207Pb

Sm-Nd and Rb-Sr isotopes

The isotopic ratios of 87Sr/86Sr, 143Nd/144Nd, and the trace element concentrations of Rb, Sr,

Sm, and Nd were measured by thermal ionization mass spectrometry on whole rock

samples. Rock powders were put in large Savillex vials and dissolved in mixtures of hot

concentrated HF-HNO3 or alternatively, mixtures of cold concentrated HF-HClO4. The

ACCEPTED MANUSCRIPT

dissolved samples were spiked with the Caltech Rb, Sr, and mixed Sm-Nd spikes

(Wasserburg et al., 1981; Ducea and Saleeby, 1998) after dissolution. Rb, Sr, and the bulk

of the REEs were separated in cation columns containing AG50W-X4 resin, using 1N to

4N HCl. Separation of Sm and Nd was achieved in anion column containing LN Spec

resin, using 0.1N to 2.5N HCl. Rb was loaded onto single Re filaments using silica gel and

H3PO4. Sr was loaded onto single Ta filaments with Ta2O5 powder. Sm and Nd were loaded

onto single Re filaments using platinized carbon, and resin beads, respectively. Mass

spectrometric analyses were carried out at the University of Arizona on an automated VG

Sector multicollector instrument fitted with adjustable 1011 W Faraday collectors and a

Daly photomultiplier (Ducea and Saleeby, 1998).

Concentrations of Rb, Sr, Sm, Nd were determined by isotope dilution, with isotopic

compositions determined on the same spiked runs. An off-line manipulation programs was

used for isotope dilution calculations. Typical runs consisted of acquisition of 100 isotopic

ratios. The mean result of ten analyses of the standard NRbAAA performed during the

course of this study is: 85Rb/87Rb = 2.61199±20. Fifteen analyses of standard Sr987 yielded

mean ratios of: 87Sr/86Sr = 0.710285±7 and 84Sr/86Sr = 0.056316±12. The mean results of

five analyses of the standard nSmb performed during the course of

this study are: 148Sm/147Sm = 0.74880±21, and 148Sm/152Sm = 0.42110±6. Fifteen

measurements of the La Jolla Nd standard were performed during the course of this study.

The standard runs yielded the following isotopicratios: 142Nd/144Nd = 1.14184±2,

143Nd/144Nd = 511853±2, 145Nd/144Nd = 0.348390±2, and 150Nd/144Nd = 0.23638±2. The

Sr isotopic ratios of standards and samples were normalized to 86Sr/88Sr = 0.1194, whereas

the Nd isotopic ratios were normalized to 146Nd/144Nd = 0.7219. The estimated analytical

±2s uncertainties for samples analyzed in this study are: 87Rb/86Sr = 0.35%,

ACCEPTED MANUSCRIPT

87Sr/86Sr = 0.0014%, 147Sm/144Nd = 0.4%, and 143Nd/144Nd = 0.0012%. Procedural blanks

averaged from five determinations were: Rb-10 pg, Sr-150 pg, Sm- 2.7 pg, and Nd - 5.5 pg.

Analytical data is presented in Table 3.

Results

Fieldwork was carried out in the vicinity of Santa Marta and El Rodadero, following a NW-

SE transect to cover the different metamorphic units of the SMS (Figures 2 -3), this work

was complemented with some regionally distributed samples.

Geochemistry of meta-igneous rocks

Twenty one whole rock samples from greenschist and amphibolites metabasic rocks of the

Concha (7), Punta Betín (7) and Rodadero (8) Formations of the SMS were selected for

geochemical analysis of major and trace elements (Figure 2-3, Table 1). As the Large Ion

Lithopile Elements (LILE) and some majors (Na, K, Ca, Mg, Rb, Ba, Sr) are susceptible to

remobilization during metamorphic processes, the interpretation of magmatic evolution

relied on the relatively inmobile High Field Strength (HFS) and transition elements (Ti, Zr,

Hf, Nb, Th, Ta, Y, Cr, P, Ni, Sc) as well as the Rare Earth Elements (REE) (Winchester and

Floyd, 1977, Pearce, 1982, 1996, Jenner, 1996, Hollings and Wymann, 2005). Results are

presented in Table 1.

Although thickness variations in the metabasic layers and observed some sill-like

relationships suggest a magmatic origin, we reviewed the protolith origin with the Zr/Ti

versus Ni diagram presented by Winchester et al. (1987). Within this diagram all the

samples present a magmatic affinity (Figure 4a), therefore the geochemical data is used to

trace the tectonomagmatic processes.

SiO2 values from the three formations are relatively similar, varying between 44.48% and

52.73%, whereas MgO values from the Concha and Punta Betin formation (7.35-12.92%)

ACCEPTED MANUSCRIPT

are higher than the Rodadero Formation (5.99% and 7.92%). The higher MgO values (>11)

in two samples are probably related to a cumulitic origin, which is also reflected in the

higher Cr contents (Wilson, 1989). The Zr/Ti versus Nb/Y marks magma fractionation and

alkalinity provides a robust way to chemically discriminate metamorphosed or altered

volcanic rocks (Winchester and Floyd, 1977, Pearce, 1996). Within this diagram the

analyzed samples classified as basalts and basaltic andesites (Figure 4b). Bivariate

diagrams that used Zr as a reference immobile element, show scatter of oxides such as

CaO, Na2O or K2O (Figure 5), whereas some elements such as Fe2O3, MgO, P2O5, TiO2

and Cr clearly correlate with Zr, confirming their less mobile behavior and the possible

existence of some magmatic differentiation.

Concha Formation

REE patterns compared to chondrite are characterized by a depleted to nearly horizontal

light rare earth element (LREE) trend (Figure 6a), whith (La/Yb)N between 0.47-1.19 and

(La/Sm)N of 0.45-0.98. They also show a weak negative Eu anomaly (Eu/Eu* = 0.68-0.99),

that is better defined in the coarse-grained amphibolites (Table 1), and attest to the role of

some plagioclase fractionation. This REE pattern is similar to either Mid-Ocean ridge

basalt (MORB) or low-K intra-oceanic arcs of the eastern Pacific (Gill, 1981). Some

anomalous Ce value may be related to remobilization during oxidation conditions (Hollings

and Wyman, 2005). Multi-element patterns normalized against MORB were plottd

following Pearce (1983, 1996). We included elements with similar behavior such and Ta

and Nb or La and Ce in order to check for consistency of the data. The amphibole-schists

are characterized by relative enrichment in LILE, particularly Th, but show a HFSE pattern

parallel to MORB, with a weak to absent Ta and/or Nb anomaly (Figure 6b).

ACCEPTED MANUSCRIPT

Ti and V contents of basic magmas usually track the oxygen activity during magmatic

evolution, and therefore can be used to identify water induced melting in subduction

settings (Shervais, 1982, Rollinson, 1993). Samples plot within the combined MORB and

back-arc basalt fields, whereas two of them are more Ti depleted and plot toward the arc

tholeiite field (Figure 7a). It is commonly considered that Th enrichment and Nb, Ta and

Hf depletion are markers of subduction related settings (Wood et al., 1980). Within this

diagram the Concha Formation samples are distributed within the MORB and volcanic arc

basalts fields (Figure 7b). This non-consevative behavior of Th is also seen within the

Th/Yb versus Nb/Yb diagram after Pearce and Peate (1995), were the basic magmatic rocks

plot outside the N-MORB field towards an oceanic arc setting (Figure 7c). Similarly in the

Ti/100-Y*3-Zr diagram from Pearce and Cann (1973) the rocks clearly plot within a

transitional volcanic arc to MORB setting (Figure 7d).

Punta Betín Formation

REE patterns are characterized by depletion in the LREE () when compared with the

Middle Rare Earth Elements (MREE), with (La/Sm)N = 0.45-0.90 (Figure 5b). The Eu

negative anomaly is well defined, with Eu/Eu* values between 0.68-0.99. This pattern is

also similar to a MORB trend. Multi-element patterns normalized against MORB from the

amphibole-schists are characterized by some enrichment in (Th) with a negative Nb and Ta

anomaly, with a LILE and HFSE depletion when compared to MORB, and the HFSE lack

any spiky behavior (Figure 6b).

In the Ti versus V plate tectonic setting discrimination diagram after Shervais (1982) the

Punta Betín Formation plots within the MORB - back-arc field, close to the limit with the

volcanic arc basalts (Figure 7a), whereas in the Wood et al. (1980) diagram the rocks

follow a trend from the MORB to the volcanic arc fields, which is marked by an

ACCEPTED MANUSCRIPT

enrichment in subduction-setting related elements such as Th, incorporated either by

sediments or crustal contamination (Figure 7b, Pearce and Peate, 1995). A subduction

enrichment is also seen in the Th/Yb versus Nb/Yb diagram (Figure 7c) after Pearce and

Peate (1995). A transitional volcanic arc - MORB character is seen when elements such as

Ti, Zr and Y are compared (Figure 7d, Pearce and Cann, 1973).

Rodadero Formation

REE patterns from the Rodadero Formation show variations in the LREE from a depleted

to a well defined enriched trend (Figure 5c). The La/YbN value varies between 0.68 and

5.06, whereas La/SmN ranges from 0.49 to 2.2. This pattern is similar to MORB and a more

enriched LREE trend that resembles arc related basalts (Tatsumi and Eggins, 1995).

Normalized trace element patterns are characterized by enrichment in Th, La, Ce with a

well defined Nb and Ta depletion (Figure 6c). A Ti anomaly although weak is well

defined. HFSE trends show some minor spiked pattern but resembling MORB and inmature

arc basalts. The different Trace element discrimination diagrams also plot along the

transition from MORB to volcanic arc (Figure 7a-7d).

Geochemistry of metasediments

Three samples from the micaceous schists Punta Betín, Cinto and Rodadero Formation

were selected for major and trace element analysis. The geochemical composition of

sediments or their metamorphic equivalents are a major provenance and tectonic setting

tracer (Taylor and McLennan, 1983, McLennan et al., 1993). Similar to the meta-igneous

rocks, relatively immobile elements such as the HFSE and the REE are the most reliable

indicators.

In general SiO2 and Al2O3contents vary between 64-72% and 11.68-17.00% respectively.

Using the immobile TiO2/Al2O3 versus Zr/Al2O3 ratios (not shown) as an indicator of the

ACCEPTED MANUSCRIPT

increase on heavy mineral compound in sandstones (Roser and Nathan, 1997), it is found that

the three samples are in fact of psamitic character. REE are commonly inmobile during

post-depositional and metamorphic processes and can be used as powerful provenance

tracers (McLennan et al., 1993). The REE pattern from the three samples (Figure 8a)

shows a similar LREE enrichment, with (La/Yb)N= 3.72-7.1 and a well defined negative Eu

anomaly with Eu/Eu* 0.54-0.59, that is a common characteristic of a crust that has

experienced crustal differentiation controlled by plagioclase fractionation. This pattern is

similar to the Post Archean Australian Shale (PAAS, Figure 8a) that represents an average

of the upper continental crust (McLennan et al., 1993).

Th/Sc values commonly trace the existence of felsic and/or mafic sources within a

sediment. The obtained values are relatively closed to one (0.82-1.19), and when compared

against a Zr/Sc ratio it plots close to the upper crust (Figure 8b). Similarly, Hf versus

La/Th relations (Figure 8C) present a well defined felsic upper crust signature (Floyd and

Laveridge, 1981).In plate tectonic discrimination diagrams that include Th-Sc-Zr or the

La/Sc versus Ti/Zr, the SMS plot within a continental island arc field which maybe similar

to Japan Sea configuration (Figure 8d, e, Bhatia and Crook, 1986).

U/Pb detrital zircon geochronology

Zircons from four samples (Figures 2-3 for sample location) were selected for detrital

geochronology. Two samples are from the Concha and Rodadero Formations in the SMS,

whereas the other two are from mica-schists from a roof pendant (sample EAM-1-48)

found within the Paleogene granitoid that separates the two major belts of the Santa Marta

Province (Tschanz et al., 1969) and the other one from the most inboard Mesozoic

metamorphic belt (San Lorenzo Schist) and. Analytical data are included in Table 3. Other

ACCEPTED MANUSCRIPT

processed schist samples did not yield any zircon crystals, and therefore could not be

analyzed.

Thirty nine zircon grains were recovered from a fine-grained muscovite-schist of the

Concha Formation (sample R14). Crystals are angular to weakly rounded suggesting

relatively short transport, and U/Th ratios are <12 as expected from magmatic zircons

(Rubatto et al., 2002). A major zircon population of 30 grains yielded ages in the range

from 80 Ma to 91 Ma, with a major peak at 82 Ma (Figure 9a). From three of these zircon

grains an older weight average age of 89.6 ± 1.9 Ma was obtained, whereas the ten

youngest grains provide a well defined 81.8±0.96 Ma average age. A single Cambrian to

Mesoproterozoic and an Early Archean grain were also recovered. Although statistically

limited (Gehrels et al., 2006), these results suggest that older continental sources were also

feeding this basin during deposition. Zircons from the Rodadero Formation (sample S8) are

also characterized by typical magmatic U/Th ratios <12 (Rubatto et al., 2002). The detrital

zircon ages span between the Middle Triassic and the Carboniferous (Figure 9b), with

major peaks at 248 Ma and 284 Ma. A youngest 206Pb/238U age of 235 ± 4 Ma was obtained

from six grains. The two major peaks with additional single Mesoproterozoic zircons that

indicate the input of the older sources. Seventy six zircons from the roof pendant within the

granitoid were analyzed (sample EAM-11-48), of which 83% are of Phanerozoic age

(n=64), with a record that spans from the Jurassic to the Cambrian (Figure 9c). A major

Early Jurassic peak of 198 Ma and a younger concordant age of ca. 160 ± 3 Ma clearly

suggests a post-Jurassic depositional age, whereas additional and representative Triassic,

Permian and Early Paleozoic peaks of 226 Ma, 265 Ma and 284 Ma are also seen (Figure

9c). Minor Grenvillian 1.05-1.2 Ga (n=5) and Paleoproteorozic signatures 1.7 Ga (n=2) are

also characteristic. The San Lorenzo Schist (sample S4) yielded relatively few zircons

ACCEPTED MANUSCRIPT

(n=15). Peaks at 157 Ma and 252 Ma are represented by three and five crystals (Figure

9d). This suggests that sedimentary deposition of the protolith took place after the Middle

Jurassic. As with other samples, grains with Mesoproterozoic ages between 1.0-1.5 Ga

were also recognized and attest to their relative importance.

Sr-Nd Isotopes

Five meta-igneous samples were selected for whole rock Rb/Sr and Sm/Nd isotopic ratio

analysis. We included greenschists and amphibolites from the Punta Betín (2) and

Rodadero Formations (1) and two coarse-grained amphibolites from the Concha Formation.

Results are presented in Table 4 and Figure 10. Values were calculated for 82 Ma (age of

the youngest detrital zircon in the Concha Formation). The five samples show a relatively

juvenile character, with positive and depleted mantle signatures, with �Nd varying between

8.62-9.51 units with additional initial 87Sr/86Sr varying between 0.70283 to 0.70375.

When compared with other Circum-Caribbean magmatic provinces and global reservoirs

(compilations after White and Hofmann, 1982, Gribble et al., 1996, Thompson, 2003, Jolly et al.,

2006, 2008), the Punta Betín and Rodadero formations present a Nd and Sr isotopic

signature that is comparable with the Caribbean primitive island arc or the Cental American

arc (Figure 9), formed by relatively normal intra-oceanic subduction.

In contrast, the Concha Formation has a MORB-type signature. This arc-MORB character

that was recognized in the geochemical data from the three formations, is similar to that

found in the relatively adjacent ca. 77 Ma Cabo de la Vela magmatic complex from the

Guajira Peninsula (Weber et al., in press). The positive �Nd data from the SMS differs

enormously from the negative or more evolved values seen Proterozoic and Paleozoic

metamorphic or the Jurassic magmatism that characterized the continental margin of South

America (Cordani et al., 2005; Ordoñez, 2002, Cardona-Molina et al., 2006, Vinasco et al.,

ACCEPTED MANUSCRIPT

2006), suggesting that the assimilation of older crust and the sedimentary input was more

restricted during magma genesis. Moreover, it also precludes the participation of enriched

mantle reservoirs common in subcontinental lithosphere or in intraplate oceanic volcanism.

Tectonomagmatic setting

Different types of mafic volcanites and ophiolite fragments have been found within the

southern margin of the Caribbean, including island arc, MORB, rift, transitional continental

and oceanic plateau remnants (reviews in Giunta et al., 2002, Thompson et al., 2004, Ostos

and Sisson, 2005, Weber et al., 2009). Their affinity and accretion have provided major

insights on the tectonic evolution of the Caribbean oceanic plate and its relation with the

South American continent. The compositional, temporal and spatial distribution of the SMS

place the within this regional tectonic context. Lithostratigraphic and metamorphic

relations, including previous observations from Doolan (1971), allow divsion of the SMS

into three major volcano-sedimentary units. The northwestern Concha Formation thrusts

over the composite Punta Betín and Cinto Formation, and the inboard Rodadero

Formations. Although lithostratigraphic characteristics from the Rodadero Formation are

similar to the other two formations, this unit acquired high amphibolite facies that contrasts

with the transitional greenschist - amphibolite facies rocks of the adjacent units

(Bustamante et al., 2009). Thermobarometrical data suggests that the relation between the

two units is tectonic (Bustamante et al., 2009).

The youngest detrital zircon age from the analyzed samples, clearly suggest that the

sedimentary protoliths for the different units, including the southeastern San Lorenzo

Schists were formed during the Mesozoic. Zircons from the Concha Formation indicate that

deposition of this formation took place after ca. 82 Ma. Whereas zircon metamorphic ages

from a coarse grain garnet-biotite schist from the Rodadero Formation as well as intrusive

ACCEPTED MANUSCRIPT

relations with Paleogene granitoids limits protolith formation and metamorphism to ca. 65

Ma (Cardona et al., submitted). Similarities in their detrital zircon signature and the

reconnaissance metasedimentary geochemistry suggest that they share a common

paleogeography during sedimentation.

As mentioned above, the petrochemical character of the Santa Marta Schists indicates a

mixed MORB to arc signature. Several geochemical evidences also distinguish the schist

protoliths from the Caribbean plateau basalts that constitute a major accreted element in

western Colombia, Ecuador and the Dutch Antilles (Kerr et al., 1997, 2002, Thompson et

al., 2003). Some of the rocks are characterized by a LREE depletion pattern similar to

MORB basalts, whereas others present a well defined Nb anomaly with an additional LREE

enrichment resembling magmas form in intra-oceanic arc related settings (Hofmann, 1988,

Pearce, 1996, Hawkesworth and Scherstén, 2007). Within the Zr/Y versus Nb/Y relations

commonly used to distinguished oceanic plateau from MORB and arc settings (Fitton et al.

1997, Thompson et al., 2004, Hastie et al., 2006), the mafic rocks of Santa Marta clearly

fall outside the Caribbean and Ontog Java plateau field (Figure 11), being more

comparable to MORB, Pacific and Caribbean intra-oceanic arc fields. Similarly Nd and Sr

isotopes also show affinity with other Caribbean intra-oceanic volcanic arc provinces.

The more inland Rodadero Formation may be characterized by an stronger arc related

signature, whereas the outer Punta Betín and Concha Formations show a mix between arc

and mid ocean ridge basalt trends. The most appropriate tectonic model depend on the

interpretation of the available temporal constrains. If all the formations were formed within

a relatively successive time interval, is possible to consider them as part of an evolving arc

to back-arc setting (Figure 12A) or as tectonic elements on the transition between the

island arc and an the oceanic crust (Figure 12b). In either cases as extension and basin

ACCEPTED MANUSCRIPT

widening proceeds or as we move away from the arc to the oceanic crust, the enriched

mantle wedge magmatic arc signature (Rodadero Formation) is being gradually replaced by

a MORB signature (Saunders and Tarney, 1984, Wilson, 1989, Taylor and Martinez, 2003,

Hollings and Wyman, 2005) as seen in the Concha and Punta Betín. To the southeast of the

SMS an orthogneissic body enclosed in the San Lorenzo Schist yielded crystallization ages

of ca. 90 Ma (Cardona et al., submitted). Within this model this element is part of the older

advancing arc front. As already discussed, all the Cretaceous rocks from the Santa Marta

region were already accreted to the continental margin by ca. 65 (Figure 13b). Within the

proposed paleogeographic configuration of these intra-oceanic elements, the metamorphism

and tectonic stacking of the different units of the SMS, reflects the closure and piling of the

back-basin as the arc was colliding in the front with the South American continent. Similar

tectonic stacking and back-arc closure tectonics are predicted in termo-mechanical

analogue experiments or in the accretion of the Banda Arc in Indonesia (Vroon et al.,

1996, Boutelier et al., 2003, Harris, 2006).

The metamorphism of the inland San Lorenzo Schist was also controlled by this accretion,

where the arc and continental margin are juxtaposed, as has been suggested by the

remobilization of the Carboniferous and older Paleozoic basement (Tschanz et al., 1969,

Cardona-Molina et al., 2006, Cardona et al., submitted),.

More complexities to this model may arise through the former K-Ar ages of ca. 110 Ma

from MacDonald et al. (1971) obtained in the coarse-grain amphibolites from the Concha

Formation. As already indicated, our attempt to date this similar amphibolites by Ar-Ar

have not yielded results, whereas the only available metamorphic ages, was found at the

Rodadero Formation by ca. 65 Ma (Cardona et al., 2009).

ACCEPTED MANUSCRIPT

However, if in fact there are some vestiges of Albian remnants incorporated in this

metamorphic pile, they could be interpreted as the remnants of older arc basement that was

probably already metamorphosed, and subsequently covered by the volcano-sedimentary

rocks associated within the younger back-arc system.

Provenance and Caribbean tectonic constrains

The geochemical characteristic from the metasedimentary rocks have shown that sediment

provenance from the SMS is principally related to a felsic and highly differentiated crust.

However additional constrains suggest that the tectonic setting for protolith deposition is

akin to a continental island arc signature, which implies a mixed setting where arc elements

and probably older sediments were feeding the basin. This is in fact similar to what is found

either in a Japan-type marginal basin or in areas where sediment dispersal patterns allow

the mix of sources derived from different tectonic settings (McLennan et al., 1990).

A similar pattern is seen within the detrital zircon record, which also suggests that all the

sedimentary units were fed by relatively similar older sources. The youngest 80-90 Ma

zircon ages within the northwestern Concha Formation, show that Cretaceous magmatic

sources were contributing to the sedimentary budget of the protoliths. These ages are

similar to the crystallization ages of an orthogneiss protoliths in the inner San Lorenzo

Schists (Cardona et al., submitted). Within the Caribbean this time span correspond to

major arc growth episode (Pindell and Keenan, 2002). It is therefore possible to link the

Cretaceous source to the erosion of a Caribbean arc.

Grenvillian age sources resemble those recorded in the eastern segment of the Colombian

Andes, including some major outcrops within the Santa Marta massif and the Guajira

Peninsula (Cordani et al., 2005, Cardona et al., 2009). The extensively Late Paleozoic to

ACCEPTED MANUSCRIPT

Triassic age population also correlates with recently identified Early Permian granitoids in

the Santa Marta region (Cardona et al., submitted to this volume) and the widespread sin-

tectonic granitoids of the Central Cordillera of the Colombian Andes (Vinasco et al., 2006,

Ibañez et al., 2008). This Late Paleozoic-Triassic belt is part of a broader series of orogens

the extend from south Peru to Venezuela and record the final stages of agglutination of

Pangea (Burkley, 1973, Noble et al., 1997, Vinasco et al., 2006, Cardona et al., 2008). The

Early to Middle Jurassic age population found within the roof pendant and the southeastern

San Lorenzo Schist are similar to the major Jurassic magmatic ages that characterized the

Northern Andes (Tschanz et al., 1974, Aspden et al., 1987, Dörr et al., 1995, Cardona-

Molina et al., 2006). Therefore the sedimentation of the sedimentary protoliths are related

to the erosion of an older continental source similar to the South American continental

margin. The extensive amount of Late Paleozoic compounds also suggest that the deeper

levels of the Pangean orogen was already exhumed and eroded since the Late Mesozoic as

seen in other segments of the Andes (Toussaint, 1996, Martín-Gombojav and Winkler,

2007). In contrast the more limited proportion of Jurassic compounds suggest that these

widespread arc rocks that cover the eastern segment of the northern Andes and that were

covered by the Cretaceous passive margin sediments were not deeply exhumed during the

Late Cretaceous.

Stratigraphical constrains have shown that contemporaneously to the growth of this

Cretaceous arc, the adjacent continental basin in the southeastern Santa Marta Massif was

characterized by tectonic quiescence until the Maastrichian (Martinez and Hernandez,

1992, Villamil, 1999). Therefore the protoliths of the Cretaceous volcanics of the Santa

Marta Province must have been formed outside of their current position (Figure 13a).

However, as previously mentioned, the strong contribution of older Paleozoic and

ACCEPTED MANUSCRIPT

Proterozoic material suggest that the block was already close to the continent (Figure 14).

Modern tectonic analogues for these volcano-sedimentary relations are found in the Lesser

Antilles or the Kermadec arcs, where the sedimentary fill of the intra-oceanic arc setting

was influenced by the discharge of the adjacent continental margins as this arc continues its

magmatic evolution in the oceans (Figure 14), or within New Guinea where the approach

to the continental margin incorporates progressively thicker continental related sediments

(Cloos et al., 2005).

Correlative intra-oceanic fragments with associated continental inputs in their sediments are

found in the Guajira Peninsula from northeastern Colombia (Weber et al., 2009), the

Netherland Antilles (Thompson et al., 2004, Wright and Wyld, 2004) and the Venezuelan

coast (Ostos and Sisson, 2005). These elements are therefore possibly related to a common

arc formed in the front of the Caribbean plate. Weber et al. (2009) have suggested that

some of these sediments may have been incorporated in the subduction channel, as this arc

approached the continent. Two major plate tectonic models have been invoke for the origin

of the Caribbean plate, an inter-Americas authocthonous origin and an allocthonous Pacific

derived Caribbean plate tectonic model (Pindell, 1993, Meschede and Frisch, 1998, Pindell

et al., 2006). In the present paper we follow the actualized Pindell et al. models, as it

integrates available Circum-Caribbean geology in a more coherent fashion. By ca. 90 Ma

the front of the Caribbean plate was migrating to the northeast and reaching the South

America continental margin (Figure 13a-b). Arc growth was already controlled by the

subduction of the proto-Caribbean ocean that separates the Americas, and is represented by

the orthogneisses and amphibolites found in the San Lorenzo Schist and probably some arc

rocks of the Santa Marta Schists (Rodadero Formation). By ca. 82 Ma back-arc basin

formation was recorded by parts of the Concha and Punta Betín Schists in the SM. Back-arc

ACCEPTED MANUSCRIPT

formation is related to the subduction of the older and already cold proto-Caribbean crust

(Sdrolias and Müller, 2006). Other triggering mechanism for back-arc basin formation may

be the oblique displacement of the Caribbean front and its expansion as it entered the larger

Proto-Caribbean basin between the American, similar to the Grenade and Yucatan openings

(Pindell and Keenan, 2002). As the arc-back-arc elements of the Caribbean plate (including

the SMS and the other schist units of Santa Marta were obliquely approaching the South

American margin, several fragments of the eastern segment of the plate were diachronously

accreted from south to north (Pindell et al., 2005, Vallejo et al., 2007, Cardona et al.,

submitted). The associated uplift of the margin generated a significant amount of

continental sediments that were discharged to the advancing portion of the Caribbean plate

and its arc front and back-arc elements as it continued it advance (Figure 14). This explains

the associated continental input found within the Santa Marta Schists protoliths and other

eastern Caribbean accreted segments. The inboard San Lorenzo Schist which is associated

with ca. 90 Ma plutonism also shows an older continental detrital input which probably

tracks the inception and approach of the Caribbean arc front to the Americas margin by that

time (Pindell et al., 2005). Although not discussed within this paper, the existence of

continental fragments derived from the previous proto-Caribbean opening, which can be

incorporated as fragments to the advancing intraoceanic arc subduction channels is an

additional complexity that can explain the existence of broader scale continental input

(Avé-Lallement and Sission, 2005).

Acknowledgments

ECOPETROL, INVEMAR and INGEOMINAS are acknowledged for providing support

during several phases of this research. Discussions and support from G. Guzman, F.

ACCEPTED MANUSCRIPT

Colmenares and the Geosearch Ltda Sierra Nevada team are highly appreciated. Comments

by two anonymous reviewer are highly appreciated Analytical work received support from

the Fundación para el Apoyo de la Investigación y la Cultura del Banco de la República de

Colombia, project 2289. Funding for the Arizona LaserChron Center is provided by NSF

EAR-0443387. This is a contribution to the IGCP 546: “Subduction zones of the

Caribbean.”

Bibliography

Aspden, J.A., McCourt, W.J., and Brook, M. 1987. Geometrical control of subduction-related

magmatism: the Mesozoic and Cenozoic plutonic history of western Colombia. Journal of

the Geological Society, London, 144, 893–905.

Avé-Lallement, H. G., Sisson, V. B., 2005. Exhumation of eclogites and blueschists in northern

Venezuela: constraints from kinematic analysis of deformation structures. In: Avé

Lallemant, H. G., Sisson, V. B. (Eds.): Caribbean-South American Plate Interactions,

Venezuela. Geological Society of America Special Paper 394, 193-206.

Bayona, G., Lamus-Ochoa, F., Cardona, A., Jaramillo, C., Montes, C., Tchegliakova, N., 2007.

Procesos orogénicos del Paleoceno para la Cuenca Ranchería (Guajira, Colombia) y áreas

adyacentes definidos por análisis de procedencia. Geología Colombiana. 32, 21-46.

Bhatia, M., Crook, K. A W., 1986. Trace element characteristics of greywackes and tectonic

setting discrimination of sedimentary basins. Contributions to Mineralogy and Petrology.

92, 181-193.

ACCEPTED MANUSCRIPT

Boutelier, D., Chemenda, A., Burgg, J-P., 2003. Subduction versius accretion of intra-oceanic

volcanic arcs insight from thermo-mechanical analogue experiments. Earth and Planetary

Science Letters. 212, 31-45

Burkley, L. A, 1976. Geochronology of the Central Venezuelan Andes. PhD. Thesis. Case

Western Reserve University. 150 p.

Cardona-Molina, A., Cordani, U., MacDonald, W., 2006. Tectonic correlations of pre-Mesozoic

crust from the northern termination of the Colombian Andes, Caribbean region. Journal of

South American Earth Sciences. 21, 337-354.

Cardona, A., García-Casco, A., Ruiz, J., Valencia, V., Bustamante, C., Garzón, A., Saldarriaga,

M., Weber, M., 2008b. Late Cretaceous Caribbean-South America interactions: insights

from the metamorphic record of the NW Sierra Nevada de Santa Marta, Colombia. 18th

Caribbean Geological Conference. Santo Domingo, República Dominicana, 24-29 March.

Abstracts and program. 12.

Cardona, A., Ruiz, J., Valencia, V., Jaramillo, C., Ojeda, G., Bayona, G., submitted to Geologica

Acta U/Pb LAM-ICP-MS zircon geochronology and whole rock geochemistry from a

biotite tonalite of the Baja Guajira basin, Colombia: tracking the Meso-Cenozoic

migration of the Caribbean plate.

Cardona, A., Ruiz, J., Valencia, V., Bayona, G., Duque, J., Jaramillo, C., Montes, C., Ojeda, G.,

submitted to Geology. Late Cretaceous to Eocene accretion and subduction in the Sierra

Nevada de Santa Marta and adjacent Rancheria basin, northernmost Colombia:

Implications for Northern Andes orogeny and Caribbean plate tectonic model.

ACCEPTED MANUSCRIPT

Cloos, M., Sapiie, B., van Ufford, A. Q., Weiland, R. J., Warren, P. Q., McMahon, T. P., 2005.

Collisional delamination in New Guinea: The geotectonics of subducting slab break-off.

Geological Society of America, Special Paper 400. 51 p.

Colletta, B., Roure, F., de Toni, B., Loureiro, D., Passalacqua, H. and Gou, Y., 1997. Tectonic

inheritance, crustal architecture and contrasting structural styles in the Venezuela Andes.

Tectonics. 16, 777-794.

Dickinson,W.R., Gehrels, G. E., 2003. U-Pb ages of detrital zircons from Permian and Jurassic

eolian sandstones of the Colorado Plateau, USA: paleogeographic implications.

Sedimentary Geology. 63, 29-66.

Cordani, U. G., Cardona, A., Jiménez, D., Liu, D., Nutman, A. P., 2005. Geochronology of

Proterozoic basement inliers from the Colombian Andes: tectonic history of remnants

from a fragmented Grenville belt. In: Vaughan, A. P. M., Leat P. T., Pankhurst, R. J.

(Eds), Terrane Processes at the Margins of Gondwana. Geological Society [London]

Special Publication 246, p. 329-346.

Doolan, B. L., 1971. Structure and metamorphism of the Santa Marta area, Colombia, South

America: Ph.D. dissertation. New York State University, Binghamton, N.Y.

Dörr, W., Grosser, J. R., Rodriguez, G. I., 1995. Zircon U-Pb age of the Paramo Rico tonalite-

granopdiorite, Santander Massif (Cordillera Oriental, Colombia) and its geotectonic

significance. Journal of South American Earth Sciences. 8, 187-194.

ACCEPTED MANUSCRIPT

Ducea, M.N., Saleeby, J.B., 1998. The age and origin of a thick mafic ultramafic root from

beneath the Sierra Nevada batholith, Contributions to Mineralogy and Petrology, v. 133,

p. 169-185.

Fitton, J.G., Saunders, A.D., Norry, M.J., Hardarson, B.S., Taylor, R.N., 1997. Thermal and

chemical structure of the Iceland plume. Earth and Planetary Science Letters 153, 197-

208.

Floyd P.A., Leveridge, B.E., 1987. Tectonic environment of the Devonian Gramscatho basin,

south Cornwall: framework mode and geochemical evidence from turbiditic sandstones.

Journal of the Geological Society of London. 144, 531-542.

Gehrels G., Valencia V., Pullen A., 2006. Detrital zircon geochronology by Laser-Ablation

Multicollector ICPMS at the Arizona LaserChron Center. In Olszewski, T.D. (Ed),

Geochronology Emerging opportunities, Paleontological Society V.12, p.67-76.

Gehrels, G., Valencia, V., Ruiz, J., 2008. Enhanced precision, accuracy, efficiency, and spatial

resolution of U-Pb ages by laser ablation-multicollector-inductively coupled plasma-mass

spectrometry. Geochemistry Geophisics Geosystems. 10.1029/2007GC001805.

Gill, J. B., 1981. Orogenic Andesites and Plate Tectonics. Berlin: Springer Verlag.

Giunta, G., Beccaluva, L., Coltorti, M., Siena, F., Vaccaro, C., 2002. The southern margin of the

Caribbean Plate in Venezuela: tectono-magmatic setting of the ophiolite units and

kinematic evolution. Lithos, 63, 19-40.

Giunta, G., M. Marroni, E. Padoa, and L. Pandolfi, 2003, Geological constraints for the

geodynamic evolution of the southern margin of the Caribbean plate, in C. Bartolini, R. T.

ACCEPTED MANUSCRIPT

Buffler, and J. Blickwede, eds., The Circum-Gulf of Mexico and the Caribbean:

Hydrocarbon habitats, basin formation, and plate tectonics: AAPG Memoir 79, p. 104–

125.

Gribble, R. F., Stern, R, J., Bloomer, S. H., Stüben, D., O’Hearn, T. & Newman, S., 1996. MORB

mantle subduction components interact to generate basalts in the southern Mariana Trough

back-arc basin. Geochimica et Cosmchimica Acta, 60, 2153-2166.

Harris, R., 2006. Rise and fall of the eastern Great Indonesian Arc recorded by the assembly,

dispersion and accretion of the Banda Terrane, Timor. Gondwana Research. 10, 207-231

Hastie, A., R. Kerr, A., Mitchell, S. F., Millar, I. L., 2008. Geochemistry and petrogenesis of

Cretaceous oceanic plateau lavas in eastern Jamaica. Lithos 101, 23–343

Hawkesworth, C.J., and Scherstén, A., 2007. Mantle plumes and geochemistry, Chemical

Geology 241, 319-331

Hofmann, A. W., 1988. Chemical differentiation of the Earth, the relationship between mantle,

continental crust and oceanic crust. Earth and Planetary Science Letters. 90, 297-314

Hollings, P., Wyman, D., 2005. The geochemistry of trace elements in igneous systems:

principles and examples from basaltic systems. En Linnen, R.L., Samson, I.M. (eds.).

Rare-Element Geochemistry and Mineral Deposits: Geological Association of Canada,

GAC Short Course Notes 17, p. 1 – 16.

Howell, D.G. 1995. Principles of Terrane Analysis: New Applications for Global Tectonics,

Chapman & Hall, New York.

ACCEPTED MANUSCRIPT

Jenner, G.A., 1996, Trace element geochemistry of igneous rocks: geochemical nomenclature and

analytical geochemistry: in Wyman, D.A., ed., Trace element geochemistry of volcanic

rocks: applications for massive sulphide exploration. Geological Association of Canada,

Short Course Notes. 12, 51-77.

Ibañez-Mejía, M., Jaramillo-Mejía, J. M., Valencia, V., 2008. U-Th/Pb zircon geochronology by

multicollector LA-ICP-MS of the Samaná Gneiss: a Middle Triassic syn-tectonic body in

the Central Andes of Colombia, related to the latter stages of Pangea assembly. VI South

American Symposium on Isotope Geology San Carlos de Bariloche – Argentina.

Extended Abstracts.

Iturralde-Vinent, M. A., Lidiak, E. G. (editors), 2006. Caribbean Plate Tectonics: Stratigraphic,

Magmatic, Metamorphic and Tectonic Events (UNESCO/IUGS IGCP Project 433).

Geologica Acta, 4, 1-341.

Jolly, W. T., Lidiak, E. G., Dickin, A. P., 2006. Cretaceous to Mid-Eocene pelagic sediment

budget in Puerto Rico and he Virgin Islands (northeast Antilles Island arc). Geologica

Acta, 4, 35-62.

Kellog, J. N., 1984. Cenozoic tectonic history of the Sierra de Perijá, Venezuela-Colombia, and

adajacent basins. Geological Society of America. In: Bonini, W. E., Hargraves, R. B.,

Shagam, R. (Eds): The Caribbean-South American plate boundary and regional tectonics.

Geological Society of America Memoir 162. 239-261.

ACCEPTED MANUSCRIPT

Kerr, A.C., Marriner, G.F., Tarney, J., Nivia, A., Saunders, A.D., Thirlwall, M.F., Sinton, C.W.,

1997. Cretaceous basaltic terranes in Western Colombia: elemental, chronological and Sr–

Nd Isotopic Constraints on petrogenesis. Journal of Petrology, v. 38, N° 6, p. 677 – 702.

Kerr, A.C., Aspden, J.A., Tarney, J., Pilatasig, L.F., 2002. The nature and provenance of accreted

oceanic terranes in western Ecuador: geochemical and tectonic constraints. Journal of the

Geological Society (London) 159, 577–594.

Kerr, A.C., White, R.V., Thompson, P.M.E., Tarney, J., Saunders, A.D., 2003. No oceanic

plateau – no Caribbean Plate? The seminal role of an oceanic plateau in Caribbean Plate

evolution. En Bartolini, C., Buffler, R.T., Blickwede, J. (eds.). The Circum-Gulf of

Mexico and the Caribbean: Hydrocarbonhabitats, basin formation, and plate tectonics.

AAPG Memoir 79, p. 126– 168.

MacDonald, W.D., Doolan, B.L., Cordani, U.G., 1971. Cretaceous – Early Tertiary metamorphic

K – Ar age values from the South Caribbean. Geological Society of America Bulletin, v.

82, p. 1381 – 1388.

Macellari, C., 1995, Cenozoic sedimentation and tectonics of the southwestern Caribbean pull-

apart basin, Venezuela and Colombia, in A. Tankard, S. Suarez, and H. Welsink, eds.,

Petroleum basins of South America: AAPG Memoir 62, p. 757–780.

Muessig, K. W. 1984. Structure and Cenozoic tectonics of the Falcón Basin, Venezuela, and

adjacent areas. In: Bonini, W. E., Hargraves, R. B., Shagam, R. (Eds.) The Caribbean-

South American plate boundary and regional tectonics. GSA Memoir 162, Boulder,

Colorado, 217-230.

ACCEPTED MANUSCRIPT

Mantle, G. W., Collins, W. J., 2008. Quantifying crustal thickness variations in evolving orogens:

correlation between arc basalt composition and Moho depth. Geology, 36; 87–90.

Martin-Gombojav, N., Winkler, W., 2008. Recycling of Proterozoic crust in the Andean Amazon

foreland of Ecuador: implications for orogenic development of the Northern Andes. Terra

Nova, 20, 22–31, 2008Martinez, J. I., Hernandez, R., 1992, Evolution and drowning of the

Late Cretaceous Venezuelan carbonate platform: Journal of South American Earth

Sciences, v. 5, 197-210

McLennan, S. M., Taylor, S. R., McCulloch, M. T., Maynard, J. N., 1990. Geochemical and Nd-

Sr isotopic composition of deep sea turbidites: Crustal evolution and plate tectonic

association. Geochimica et Cosmochimica Acta. 54, 2015-2050

McLennan, S. M., Hemming, S., McDaniel, D. K., Hanson, G. N., 1993. Geochemical

approaches to sedimentation, provenance and tectonics. Geological Society of America,

Special Paper 284. 21-40.

Meschede, M., Frisch, M., 1998. A plate-tectonic model for the Mesozoic and early Cenozoic

history of the Caribbean Plate. Tectonophysics, 296, 269-291.

Montes, C., Hatcher, R.D. & Restrepo-Pace, P., 2005. Tectonic reconstruction of the northern

Andean blocks: Oblique convergence and rotations derived from the kinematics of the

Piedras–Girardot area, Colombia. Tectonophysics, 399, 221-250.

Noble, S. R., Aspden, J. A, Jemelita, R., 1997. Northern Andean crustal evolution: New

U-Pb geochronologial constraints from Ecuador. Geological Society of America

Bullettin, 109, 789-798.

ACCEPTED MANUSCRIPT

Ordoñez, O., 2001. Caracterização isotópica Rb-Sr e Sm-Nd dos principais eventos magmáticos

nos Andes Colombianos. Tesse de Doutoramento Universidade de Brasilia. 197 p

Ordoñez, O, Pimentel, M., 2002. Rb-Sr and Sm-Nd isotopic study of the Puquí complex,

Colombian Andes. Journal of South American Earth Sciences. 15, 175-182.

Ostos, M., Sisson, N., 2005. Geochemistry and tectonic setting of igneous and metaigneous rocks

of northern Venezuela. In: Avé Lallemant, H. G., Sisson, V. B. (Eds.): Caribbean-South

American Plate Interactions, Venezuela. Geological Society of America Special Paper

394, 119-156

Pearce, J. A., Cann, J. R., 1973. Tectonic setting of basic volcanic rocks determined using trace

element analyses. Earth and Planetary Science Letters, 19. 290-300.

Pearce, J.A., and Peate, D.W., 1995, Tectonic implications of the composition of volcanic arc

magmas: Annual Review of Earth and Planetary Science Letters, v.23, p. 252-285.

Pearce, J.A., 1996. A user´s guide to basalt discrimination basalts. En Wyman, D.A. (ed). Trace

Element Geochemistry of Volcanic Rocks: Applications for Massive Sulphide

Exploration. Geological Association of Canada, Sort Course Notes, v.12, p. 79 – 113.

Pindell, J. L., 1993, Evolution of the Gulf of Mexico and the Caribbean, in S. K. Donovan and

T.A. Jackson (eds.), Caribbean Geology: An Introduction. University of the West Indies

Publisher's Association 13-39.

Pindell, J. L., Kennan, L., 2001. Kinematic evolution of the Gulf of Mexico and Caribbean.

Transactions, Petroleum systems of deep-water basins: global and Gulf of Mexico

ACCEPTED MANUSCRIPT

experience. GCSSEPM 1st Annual Research Conference, Houston, Texas, G CSSEPM,

159-192.

Pindell, J., Kennan, L., Maresch, W. V., Stanek, K. –P., Draper, G., Higgs, R., 2005. Plate

Kinematic and crustal dynamics of circum-Caribbean arc-continent interactions: Tectonics

controls on basin development in the Proto-Caribbean margins. In: Avé Lallemant, H. G.,

Sisson, V. B. (eds.): Caribbean-South American Plate Interactions, Venezuela. Geological

Society of America special paper 394, 7-52

Pindell, J. L., Kennan, L., Stanek, K. P., Maresch, W. V. & Draper, G., 2006. Foundations of

Gulf of Mexico and Caribbean evolution: eight controversies resolved. Geologica Acta, 4,

303-341.

Rabe, 1977. Zur Stratigraphie des ostandinen Raumes von Kolumbien. Giessner Geologishe

Schriften. 223p.

Restrepo-Moreno, S., Foster, D: Kamenov, G., 2007. Formation age and magma sources for the

Antioqueño Batolith derived from LA-ICP-MS Uranium-Lead dating and Hafnium-

isotope analysis of zircon grains. Geological Society of America Denver Annual Meeting.

Paper No. 181-28.

Rollinson, H.R., 1993. Using Geochemical Data: Evaluation, Presentation, Interpretation.

Prentice Hall, Singapore, 352 p.

Roser, B. P., Nathan, S., 1997. An evaluation mobility during metamorphism of a turbidite

sequence (Greenland Group, New Zealand). Geological Magazine. 134, 219-244.

ACCEPTED MANUSCRIPT

Rubatto D., 2002. Zircon trace element geochemistry: distribution coefficients and the link

between U-Pb ages and metamorphism. Chemical Geology. 184, 123-138.

Saunders, A. D., Tarney, J., 1984. Geochemical characteristics of basaltic volcanism within back-

arc basin. In: Marginal basin geology: volcanic associated sedimentary and tectonic

processes in modern and ancient marginal basins. Eds: B. P. Kokelaar and M. F. Howells.

Geological Society of London, Special Publication 16. 59-76.

Sdolian, M., Müller, D. R., 2006. Controlos on back-arc basin formation. Geochemistry

Geophysics Geosystems 7. Q04016, doi:10.1029/2005GC001090.

Shervais, J. W., 1982. Ti-V plots and the petrogenesis of modern and ophiolitic lavas. Earth and

Planetary Science Letters, 59, 101-118.

Shervais, J. W., 2001. Birth, death, and resurrection: The life cycle of suprasubduction zone

ophiolites. Geochemistry, Geophysics, Geosystems. 2. 2000GC000080

Sengör, A.M.C., Natal'in, B.A., 1996. Turkic-type orogeny and its role in the making of the

continental crust. Annuals Reviews in Earth and Planetary Science Letters, 24, 263-337.

Sisson, V. B., Avá Lallemant, H. G., Ostos, M., Blythe, A. E., Snee, L. W., Copeland, P., Wright,

J. E., Donelick, R. A., Guth, L. R. 2005. Overview of radiometric ages in three

allochthonous belts of northern Venezuela: Old ones, new ones, and their impact on

regional geology. In: Avé Lallemant, H. G., Sisson, V. B. (Eds.): Caribbean-South

American Plate Interactions, Venezuela. Geological Society of America Special Paper

394, 91-118

ACCEPTED MANUSCRIPT

Smith, I. E. M., Wothington, T. J., Stewart, R. B., Prices, R: C., Gamble, J. A., 2003. Felsic

volcanism in the Kermadec acr, SW Pacific: crustal recycling in an oceanic setting.

Geological Society, London, Special Publications 219. 99-118.

Stacey, J.S., Kramers, J.D. 1975. Approximation of the terrestrial lead isotope evolution

by a two-stage model. Earth and Planetary Science Letters, 26, 207-221.

Stöckhert, B., Maresch, W. V., Brix, M., Kaiser, C., Toetz, A, Kluge, R, Krückhans-Lueder,

G., 1995. Crustal history of Margarita Island (Venezuela) in detail: Constrains on the

Caribbean plate-tectonic scenario. 23, 787–790.

Taboada, A, Rivero, L., Fuenzalida, A, Cisternas, A, Philip, H., Bijwaard, Olaya, J, Rivera, C.,

2000. Geodynamics of the northern Andes: Subduction and intracontinental deformation

(Colombia). Tectonics. 19, 787-813.

Tatsumi, Y., Eggins, S., 1995. Subduction zone magmatism. 211p.

Taylor, S. R., MacLennan, S. M., 1985. The continental crust. Blackwell, Oxford. 312p.Taylor,

B., Martinez, F., 2003. Back-arc basin basalt systematics. Earth and Planetary Science

Letters, 210, 280-297.

Thompson, P.M.E., Kempton, P.D., White, R.V., Kerr, A.C., Tarney, J., Saunders, A.D., Fitton,

J.G., McBirney, A., 2004. Hf – Nd isotope constraints on the origin of the Cretaceous

Caribbean plateau and it relationship to the Gálapagos plume. Earth and Planetary

Sciences Letters, v. 217, p. 59 – 75.

Toussaint, J. F., 1996. Evolución geológica de Colombia. Cretácico. Universidad Nacional

de Colombia. Medellín. 277 p.

ACCEPTED MANUSCRIPT

Tschanz, C.M., Jimeno, A., Vesga, C., 1969. Geology of the Sierra Nevada de Santa Marta area

(Colombia). Instituto de Investigaciones e Información Geocientífica, Minero – Ambiental

y Nuclear. República de Colombia. 288 p.

Tschanz, C., Marvin, R., Cruz, J., Mehnert, H., Cebula, E., 1974. Geologic evolution of the Sierra

Nevada de Santa Marta. Geological Society of America Bulletin, v. 85, p. 269-276.

Villamil, T., 1999. Campanian-Miocene tectonostratigraphy, depocenter evolution and basin

development of Colombia and Western Venezuela. Palaeogeography, Palaeoclimatology,

Palaeoecology. 153, 239-275.

Vinasco, C. J., Cordani, U. G., González, Weber, M., Pelaez, C., 2006. Geochronological,

isotopic, and geochemical data from Permo-Triassic granitic gneisses and granitoids of the

Colombian Central Andes. Journal of South American Earth Sciences. 21, 355-371.

Vroon, Z., Van Bergen, M. J., Forde, E. J., 1996. Pb and Nd isotope constraints on the

provenance of tectonically dispersed continental fragments in east Indonesia

Geological Society, London, Special Publications 106. 445-453.

Wasserburg GJ, Jacobsen SB, DePaolo DJ, McCulloch MT, and Wen T., 1981, Precise

determination of Sm/Nd ratios, Sm and Nd isotopic abundances in standard solutions,

Geochim. Cosmochim. Acta, v. 45, p. 2311-2323.

Weber, M. B. I., Cardona, A., Paniagua, F., Cordani, U., Sepúlveda, L, Wilson, R., in press. The

Cabo de la Vela mafic-ultramafic complex, Northeastern Colombian Caribbean region –

A record of multi stage evolution of a Late Cretaceous intra-oceanic arc. Special

Publication Geological Society of London.

ACCEPTED MANUSCRIPT

White, W. M., Hoffman A. W., 1982. Sr and Nd isotope geochemistry of oceanic basalts and

mantle evolution. Nature, 296, 821-825.

White, R.V., Tarney, J., Kerr, A.C., Saunders, A.D., Kempton, P.D., Pringle, M.S., Klaver,

G.Th., 1999. Modification of an oceanic plateau, Aruba, Dutch Caribbean: implications

for the generation of continental crust. Lithos 46, 43– 68.

Wilson, M., 1989. Igneous petrogenesis, a global approach. Chapman & Hall, London. 466 p.

Winchester, J. A. & Floyd, P. A., 1977. Geochemical discrimination of different magma series

and their differentiation products using immobile elements. Chemical Geology, 20, 325-

343.

Winchester, J. A., Max, M. D., Long, C. B., 1987. Trace element correlation in the reworked

Proterozoic Dalradian metavolcanic suites of the western Ox Mountains and NW Mayo

inliers, Ireland. In: Pharaoh, T., Beckinsale, R. D., Rickard, D., Geochemistry and

mineralization of Proterozoic Volcanic suites. Geologcal Society, London, Special

Publication 33. 489-502.

Wood, D.A., 1980. The application of the Th – Hf – Ta diagram to problems of tectonomagmatic

classification and to establishing the nature of crustal contamination of basaltic lavas of

the British Tertiary Volcanic Province. Earth and Planetary Science Letters, v. 50, p. 11 –

30.

Wright, J. E., Wyld, S. J., 2004. Aruba and Curacao: Renants of a collided Pacific Oceanic

Plateau? Initial Geologic results from the BOLIVAR Project: EOS Transactionas

American Geophysical Union 85 (47), Fall Meeting, Suppl., Abstract T33b-1367.

ACCEPTED MANUSCRIPT

Figures Captions

Figure 1. Distribution of accreted Mesozoic oceanic domains in northern South America

and the Circum-Caribbean region. Arc remnants and Oceanic plateau are highlighted.

Figure 2. Geological configuration of the Sierra Nevada de Santa Marta and the studied

Cretaceous units. A. Physiographic domains of northern South America. SM= Santa Marta

Massif, PR= Perija Range, BGB= Baja Guajira Basin, GS= Guajira Serranias. B.

Geological map of the Santa Marta massif region including the Cretaceous Schists

(Modified from Tschanz et al., 1969). The location of two of the samples analyzed for U/Pb

LAM-ICP-MS is included.

Figure 3. Geology of the Santa Marta Schists and the sampled areas (modified from

Doolan, 1970). Samples are highlighted.

Figure 4. A. Discrimination of volcanic and sedimentary amphibolites (Winchester and

Floyd, 1987). B. Classification volcanic rocks using relatively inmobile elements

(Winchester and Floyd, 1977). Circles= Concha Formation, Squares= Punta Betín

Formation, Filled Squares= Rodadero Formation.

Figure 5. Bivariate plots using Zr as an immobile reference element. Same symbols as in

figure 4.

Figure 6. Rare earth element concentrations normalized to chondrite and multi-elemental

diagrams normalized to MORB. A-B. Concha Formation, C-D. Punta Betín Formation, E-

F. Rodadero Formation. Same symbols as in figure 4.

Figure 7. Tectonic setting discrimination diagrams. A. Ti vs V after Shervais (1982). B.

Th-Hf/3-Ta (Wood et al., 1980). C. Th/Yb vs Nb/Yb (Pearce and Peate, 1995). D. Zr-

Ti/100-Y*3 (Pearce and Cann, 1973). Same symbols as in figure 4.

ACCEPTED MANUSCRIPT

Figure 8. A. REE patterns of selected metasedimentary rocks of the Santa Marta Schists

normalized to Chondrite. The post-Archean Australian Shale is included for comparison

after Taylor and McLennan (1985). B. Th/Sc vs Zr diagram after McLennan et al (1993).

C. Hf vs La/Th (Floyd and Laveridge, 1981). D. Sandstone geochemical discrimination

diagram (Bhatia and Crook, 1983).

Figure 9. U/Pb LAM-ICP-MS detrital zircons results from the Santa Marta and San

Lorenzo Schists. A. Concha Formation. B. Rodadero Formation. C. San Lorenzo Roof

Pendant. D. San Lorenzo Schists.

Figure 10. �Nd vs 87Sr/86Sr diagram from the Santa Marta Schists (fields after White and

Hofmann, 1982, Gribble et al., 1996, Thompson, 2003, Jolly et al., 2006, 2008).

Figure 11. Nb/Y vs Zr/Y magmatic discrimination diagram for oceanic plateau basalts

(Fitton et al., 1997).

Figure 12. Tectonic setting of the Santa Marta Schist protoliths A. Back-arc basin

model for the Santa Marta Schists (after Taylor and Martinez, 2003). B. Transition between

arc and oceanic crust.

Figure 13. Paleotectonic reconstructions for the Late Cretaceous after Pindell and Keenan

(2001). A. 100-80 Ma arc and back-arc growth in proximity to the continental margin. B.

Accretion of the Caribbean arc-front including the Santa Marta and San Lorenzo Schists.

Figure 14. Origin of the bimodal continental - intra-oceanic signature from the Cretaceous

volcano-sedimentary protoliths of the Santa Marta Massif. PCC= Proto-Caribbean crust,

CA= Caribbean arc, BA= Back-Arc basin, AR= remnant arc?, CB= Caribbean plate.

ACCEPTED MANUSCRIPT Figure 1

ACCEPTED MANUSCRIPT Figure 2

ACCEPTED MANUSCRIPT Figure 3

ACCEPTED MANUSCRIPT Figure 4

ACCEPTED MANUSCRIPT Figure 5

ACCEPTED MANUSCRIPT Figure 6

ACCEPTED MANUSCRIPT Figure 7

ACCEPTED MANUSCRIPT Figure 8

ACCEPTED MANUSCRIPT Figure 9

ACCEPTED MANUSCRIPT Figure 10

ACCEPTED MANUSCRIPT Figure 11

ACCEPTED MANUSCRIPT Figure 12

ACCEPTED MANUSCRIPT Figure 13

ACCEPTED MANUSCRIPT Figure 14

ACCEPTED MANUSCRIPT Sample 20 20 – A 22 26 MC 29 – A MC 48 – B MC 6 – A MC 10 – B MC 12 – A MC 15 – A

Rock Type Amph Amph Amph Amph Act. Schist Act. Schist Amph Amph Act. Schist Chl. Schist

Formation Concha Concha Concha Concha Concha Concha P. Betín P.Betín P.Betín P.Betín

SiO2 51.16 48.90 51.93 47.68 47.71 45.00 47.38 48.92 48.33 44.48

Al2O3 13.81 15.58 13.28 15.71 15.69 16.94 15.63 14.17 14.91 14.79

Fe2O3 7.60 8.21 7.27 5.17 9.46 10.34 9.18 11.25 12.17 8.67

MgO 8.18 8.22 9.62 12.92 10.27 10.43 7.35 9.98 9.35 7.86

MnO 0.08 0.09 0.13 0.09 0.21 0.22 0.14 0.16 0.19 0.17

CaO 12.76 12.83 12.00 14.55 8.04 8.88 13.51 9.54 8.01 9.52

Na2O 3.00 2.80 2.67 1.19 3.58 2.78 2.31 2.63 2.07 1.40

K2O 0.11 0.18 0.08 0.07 < 0.04 0.04 0.15 0.19 0.21 0.40

TiO2 1.24 1.13 0.43 0.23 1.19 0.95 1.18 1.23 1.47 0.94

P2O5 0.11 0.03 0.03 0.01 0.08 0.06 0.12 0.10 0.11 0.08

Cr2O3 0.050 0.046 0.053 0.180 0.049 0.056 0.047 0.033 0.035 0.044

LOI 1.9 2.0 2.4 2.2 3.7 4.3 3.0 1.8 3.0 11.5

Total 100.02 100.03 99.91 100.04 100.03 100.02 100.02 100.02 99.87 99.87

Ba 16.8 26.8 11.3 11.9 2.4 6.4 20.0 25.7 45.1 174.5

Co 32.7 29.7 33.1 38.9 40.2 47.1 40.9 40.2 40.0 33.7

Cs 0.1 0.2 0.1 0.1 < 0.1 < 0.1 0.1 0.3 0.3 0.4

Ga 14.2 16.4 11.7 10.5 14.1 14.3 16.2 15.5 17.9 13.1

Hf 2.1 2.1 0.6 < 0.5 1.8 1.3 2.1 1.8 2.5 1.9

Nb 2.2 2.0 < 0.5 < 0.5 1.9 1.0 1.6 1.2 1.6 2.2

Rb 2.0 3.2 1.3 2.1 < 0.5 < 0.5 2.7 4.1 5.4 11.6

Sn 1 1 < 1 < 1 1 1 1 1 1 1

Sr 111.7 138.1 99.2 116.6 133.1 150.4 150.8 112.1 96.1 128.8

Ta 0.1 0.1 < 0.1 < 0.1 0.1 < 0.1 0.1 0.1 0.1 0.2

Th 0.3 0.3 0.2 0.1 0.2 0.1 0.3 0.2 0.2 0.7

U 0.3 0.1 0.1 0.1 0.2 0.1 0.2 0.3 0.1 0.3

V 314 271 208 136 270 228 266 312 342 192

W 3.7 0.7 0.5 0.2 0.3 0.2 0.1 0.1 0.1 0.1

Zr 73.6 62.6 14.5 6.9 63.2 45.5 69.2 68.3 79.6 65.9

Y 28.3 30.1 12.2 6.3 26.4 22.6 26.0 30.0 33.8 23.7

Cr 344 316.48 364.64 1238.4 337.12 385.3 323.36 227.04 240.8 302.7

Ti 7431.3 6772.1 2576.9 1378.4 7131.7 5693.3 7071.7 7371.4 8809.7 5633.42

La 3.1 2.7 1.0 1.1 2.6 1.4 2.6 2.1 1.9 3.5

Ce 8.9 7.9 2.4 1.3 7.8 5.1 8.0 7.5 8.4 10.1

Pr 1.60 1.48 0.43 0.26 1.36 0.93 1.43 1.41 1.60 1.65

Nd 8.4 8.2 2.5 1.7 6.9 5.1 8.1 7.6 8.5 9.0

Sm 3.1 3.0 1.0 0.7 2.51 1.94 2.7 2.9 3.4 2.55

Eu 1.03 0.89 0.47 0.29 1.08 0.81 1.03 0.90 1.16 0.77

Gd 4.09 4.12 1.72 0.93 3.44 2.81 3.89 4.29 4.50 3.20

Tb 0.82 0.82 0.35 0.19 0.71 0.57 0.77 0.87 0.91 0.66

Dy 4.88 5.33 2.14 1.18 3.95 3.25 4.45 5.22 5.79 3.73

Ho 0.92 0.97 0.42 0.21 0.81 0.67 0.83 0.99 1.14 0.83

Er 3.03 3.22 1.37 0.67 2.48 2.06 2.88 3.18 3.67 2.47

Tm 0.44 0.46 0.22 0.10 0.35 0.29 0.40 0.51 0.58 0.37

Yb 2.76 2.90 1.17 0.63 2.39 2.03 2.51 2.82 3.44 2.14

Lu 0.43 0.45 0.19 0.09 0.35 0.31 0.39 0.46 0.55 0.32

Ni 12.4 22.1 23.2 36.8 111.5 153.4 47.6 29.7 60.0 98.2

Sc 39 37 43 34 39 37 36 40 43 31

(La/Sm)n 0.62 0.56 0.62 0.98 0.65 0.45 0.60 0.45 0.35 0.86

(La/Yb)n 0.76 0.63 0.58 1.19 0.74 0.47 0.70 0.51 0.38 1.11

MC 17 – A MC 57 – A MC 62 – B Cinto 4 Cinto 6 R – 15 MC 34 – A MC 44 – F MC 46 – B MC 49 – C MC 53 – A Act. Schist Act. Schist Amph Amph. Schist Amph. Schist Amph. Schist Amph Amph Amph. Schist Amph Amph

P.Betín P.Betín P.Betín Rodad Rodad Rodad Rodad Rodad Rodad Rodad Rodad48.75 42.27 49.54 47.55 50.26 50.91 49.36 52.73 47.58 48.93 46.08 15.46 15.80 14.99 16.81 15.56 16.67 14.94 12.36 14.70 16.69 17.82 9.35 8.87 10.63 10.30 10.12 8.84 11.65 9.40 12.43 9.66 9.50 8.36 9.09 8.10 6.79 7.21 6.15 5.99 11.00 7.92 6.94 7.92 0.17 0.14 0.17 0.17 0.15 0.19 0.19 0.21 0.22 0.14 0.21

10.52 11.43 10.92 14.45 12.75 11.82 11.24 10.03 11.61 12.42 14.11 2.66 1.48 3.06 0.93 0.69 3.09 3.54 1.14 2.11 2.12 2.510.07 1.00 0.20 0.36 0.56 0.41 0.47 0.49 0.49 0.55 0.45 1.04 0.99 1.52 1.41 1.21 0.96 1.85 0.67 1.87 1.24 0.87 0.10 0.09 0.14 0.20 0.14 0.09 0.15 0.14 0.13 0.11 0.12

0.045 0.051 0.032 0.052 0.050 0.055 0.035 0.093 0.026 0.044 0.0513.5 8.8 0.7 0.8 1.3 0.8 0.6 1.7 0.9 1.1 0.4

100.03 100.03 100.02 99.84 100.01 100.02 100.04 99.98 99.99 99.96 100.068.0 258.8 22.9 308.1 97.3 94.9 44.7 247.8 250.9 393.1 26.4

32.2 38.4 41.6 42.2 40.0 37.5 37.9 30.0 45.2 42.5 44.80.1 0.4 0.2 1.4 1.5 0.6 0.3 0.7 0.3 0.6 0.4

15.2 13.5 16.0 18.3 16.4 15.6 14.8 16.3 18.3 16.9 13.21.7 1.6 2.6 2.3 2.3 2.1 3.0 2.1 3.1 2.3 1.71.0 1.4 1.4 2.8 1.5 2.0 2.1 2.2 2.8 3.0 1.10.5 22.2 1.7 10.3 23.4 6.0 2.7 14.0 6.9 8.5 3.41 1 1 2 3 3 2 2 1 2 1

158.3 139.7 122.9 292.1 385.9 172.2 154.4 295.8 157.8 239.8 191.5< 0.1 < 0.1 0.1 0.2 0.1 0.1 0.1 0.2 0.2 0.2 < 0.10.1 < 0.1 0.1 0.3 0.4 1.1 0.2 2.2 0.3 0.4 0.1

< 0.1 0.1 0.9 0.2 0.3 1.0 0.1 0.5 0.4 0.9 0.1268 254 347 288 274 247 334 255 384 268 2190.2 0.3 0.2 1.1 0.5 0.2 0.2 0.1 0.2 0.1 0.3

55.6 52.0 82.3 92.8 77.0 67.2 110.1 68.0 108.1 72.7 58.926.3 24.7 34.9 32.2 26.3 28.3 37.8 19.0 38.5 30.7 25.1

309.6 350.9 220.16 357.76 344 378.4 240.8 639.84 178.88 302.7 350.96232.7 5933.1 9109.4 8450.1 7251.5 5753.3 11087.05 4015.3 11206.9 7431.3 5213.9

1.8 1.8 2.3 5.2 3.2 8.2 3.8 13.1 3.9 3.9 2.36.5 6.3 8.8 11.2 10.3 19.5 12.6 25.7 12.7 9.7 6.7

1.14 1.14 1.65 2.01 1.80 3.27 2.13 3.75 2.25 1.64 1.146.6 6.4 9.6 10.2 9.8 14.8 11.3 15.7 11.5 9.2 6.1

2.33 2.28 3.5 3.6 3.2 3.8 3.63 3.7 4.1 3.14 2.200.94 0.98 1.16 1.19 1.07 1.24 1.42 1.00 1.37 1.15 0.913.27 3.16 4.92 4.69 4.06 4.32 4.97 3.76 5.66 3.97 3.030.68 0.64 1.01 0.92 0.81 0.85 1.02 0.62 1.13 0.84 0.643.88 3.60 6.05 5.63 4.55 4.71 5.64 3.48 6.51 4.91 3.550.78 0.78 1.16 1.03 0.91 0.92 1.17 0.63 1.28 1.05 0.772.40 2.33 3.60 3.48 2.83 2.82 3.47 1.97 4.11 3.18 2.290.34 0.33 0.53 0.48 0.41 0.40 0.50 0.29 0.63 0.45 0.322.36 2.19 3.40 3.04 2.48 2.42 3.41 1.76 3.69 2.79 2.310.35 0.32 0.51 0.46 0.38 0.36 0.51 0.27 0.57 0.42 0.3343.5 104.9 26.0 37.8 39.7 19.6 17.9 28.4 20.7 59.5 44.838 34 42 39 39 36 42 43 44 35 34

0.48 0.49 0.41 0.90 0.62 1.35 0.65 2.21 0.59 0.78 0.650.52 0.56 0.46 1.16 0.88 2.30 0.76 5.06 0.72 0.95 0.68

ACCEPTED MANUSCRIPT

Sample MC 16 – A MC 22 – A MC 19 – A Rock Type Biot Schist Musc Schist Quartz SchistFormation P.Betín Cinto Rodad

SiO2 70.32 64.72 72.70Al2O3 13.00 16.85 11.68Fe2O3 6.95 6.41 4.06MgO 1.47 1.38 1.73MnO 0.04 0.11 0.06CaO 0.70 1.01 2.46Na2O 1.55 1.43 1.59K2O 1.81 3.81 2.52TiO2 0.62 0.83 0.55P2O5 0.15 0.17 0.12Cr2O3 0.009 0.012 0.009LOI 3.2 2.9 2.3

Total 99.82 99.63 99.78Ba 312.1 2039.4 611.1Be 1 1 1Co 9.4 7.4 7.1Cs 2.4 19.6 2.2Ga 14.6 21.7 12.0Hf 6.7 6.4 6.6Nb 12.0 16.8 9.2Rb 85.2 199.7 81.4Sn 3 4 2Sr 65.6 141.6 104.1Ta 0.8 1.3 0.6Th 13.1 15.9 7.4U 2.7 4.3 1.9V 84 157 68W 3.8 4.1 0.7Zr 231.0 214.0 249.6Y 29.7 44.5 22.3La 29.4 22.1 19.3Ce 63.2 43.8 42.5Pr 8.05 6.77 5.25Nd 30.5 28.3 21.1Sm 6.04 6.40 4.39Eu 1.15 1.38 0.88Gd 5.38 6.56 3.67Tb 0.95 1.31 0.67Dy 5.04 7.31 3.68Ho 1.02 1.46 0.68Er 2.94 4.59 2.19Tm 0.47 0.66 0.33Yb 2.76 4.01 2.18Lu 0.42 0.59 0.31Pb 10.3 3.5 6.1Ni 18.6 18.6 24.0Sc 11 16 9

ACCEPTED MANUSCRIPT

Analysis U 206Pb U/Th 207Pb* ± 206Pb* ± error 206Pb* ± 207Pb* ± 206Pb* ± Best age ±(ppm) 204Pb 235U (%) 238U (%) corr. 238U (Ma) 235U (Ma) 207Pb* (Ma) (Ma) (Ma)

S4-1 179 5734 0.8 0.31214 4.1 0.04004 1.2 0.30 253.1 3.1 275.8 10.0 473.4 86.9 253.1 3.1S4-2 696 67854 3.3 3.30037 3.5 0.24812 1.6 0.46 1428.8 20.6 1481.1 27.1 1556.9 58.0 1556.9 58.0S4-3 419 4259 1.2 0.16905 3.2 0.02426 1.0 0.31 154.5 1.5 158.6 4.7 219.9 69.7 154.5 1.5S4-5 456 14770 2.6 0.27165 3.5 0.03846 2.4 0.70 243.3 5.8 244.0 7.6 251.2 57.7 243.3 5.8S4-4 488 13620 8.8 0.25915 7.7 0.03737 1.9 0.24 236.5 4.3 234.0 16.2 208.4 174.3 236.5 4.3S4-6 434 72019 2.7 1.91934 3.9 0.17938 1.8 0.47 1063.6 17.9 1087.8 25.7 1136.7 67.5 1136.7 67.5S4-7 253 9589 3.2 1.70366 3.4 0.16283 3.0 0.88 972.5 27.5 1009.9 22.1 1092.0 32.5 1092.0 32.5S4-8 514 12840 1.5 0.17931 2.3 0.02434 1.3 0.54 155.0 1.9 167.5 3.6 347.0 44.3 155.0 1.9S4-9 677 7724 6.9 0.80497 2.2 0.09390 1.8 0.82 578.6 9.8 599.6 9.8 680.0 26.2 578.6 9.8

S4-10 505 5558 2.0 3.60108 5.5 0.27461 4.1 0.74 1564.1 56.9 1549.8 44.0 1530.2 70.1 1530.2 70.1S4-11 318 6569 1.9 0.27541 3.3 0.03944 2.9 0.87 249.4 7.1 247.0 7.3 224.5 37.5 249.4 7.1S4-12 330 6520 3.5 0.29467 4.3 0.04003 3.4 0.78 253.0 8.3 262.2 9.9 345.1 60.5 253.0 8.3S4-13 353 38955 2.2 1.74647 3.9 0.17252 3.6 0.91 1026.0 34.2 1025.9 25.5 1025.5 32.7 1025.5 32.7S4-14 506 2245 0.8 0.18476 9.7 0.02610 3.2 0.33 166.1 5.3 172.1 15.4 256.2 211.7 166.1 5.3S4-15 208 25333 1.8 2.19838 5.2 0.19114 4.4 0.85 1127.6 45.4 1180.5 36.3 1278.9 54.0 1278.9 54.0S4-16 427 8644 0.8 0.17808 4.3 0.02606 3.5 0.81 165.9 5.7 166.4 6.6 174.1 59.0 165.9 5.7S4-17 318 3687 1.6 0.16605 3.9 0.02435 2.4 0.62 155.1 3.7 156.0 5.7 169.7 72.5 155.1 3.7S4-18 572 18569 17.8 1.84188 4.4 0.16324 4.0 0.91 974.7 36.0 1060.5 28.8 1241.6 35.9 1241.6 35.9

EAM-1148-1 1211 6210 1.7 0.4583 8.8 0.0589 8.7 0.98 369.0 31.1 383.1 28.2 468.7 36.7 369.0 31.1EAM-1148-2 474 1825 5.5 0.3739 8.8 0.0471 6.9 0.79 296.8 20.1 322.6 24.4 512.9 119.9 296.8 20.1EAM-1148-4 457 3960 2.7 0.6561 5.4 0.0778 4.7 0.87 483.0 21.9 512.2 21.8 644.8 57.7 483.0 21.9EAM-1148-5 266 1090 16.6 0.2830 18.3 0.0350 7.7 0.42 221.5 16.8 253.0 41.0 556.4 364.7 221.5 16.8EAM-1148-6 1087 2225 6.2 0.2375 7.5 0.0301 4.2 0.56 191.0 8.0 216.4 14.7 502.5 137.5 191.0 8.0EAM-1148-7 454 1640 10.7 0.3072 11.0 0.0408 2.5 0.23 258.0 6.3 272.0 26.3 394.0 241.6 258.0 6.3EAM-1148-9 1047 6755 1.9 0.5883 8.5 0.0734 8.3 0.98 456.3 36.6 469.8 32.0 535.9 40.7 456.3 36.6EAM-1148-8 1071 2950 3.1 0.2878 4.7 0.0390 3.5 0.74 246.5 8.4 256.8 10.6 352.5 70.9 246.5 8.4

EAM-1148-12 900 15630 2.2 1.5838 2.9 0.1585 2.0 0.67 948.5 17.4 963.9 18.3 999.1 44.2 999.1 44.2EAM-1148-13 1232 4180 2.5 0.2272 4.0 0.0316 3.1 0.78 200.3 6.2 207.9 7.5 294.7 57.0 200.3 6.2EAM-1148-14 1228 5375 3.3 0.5552 7.6 0.0571 6.9 0.90 358.1 23.9 448.4 27.6 942.5 68.4 358.1 23.9EAM-1148-15 4487 7420 2.1 0.2530 2.7 0.0358 1.6 0.60 226.6 3.6 229.0 5.5 253.6 49.4 226.6 3.6EAM-1148-16 1307 4695 2.4 0.2827 9.0 0.0370 8.7 0.96 234.1 19.9 252.8 20.1 429.4 53.1 234.1 19.9EAM-1148-17 591 2035 3.2 0.3475 8.7 0.0430 8.1 0.93 271.6 21.6 302.8 22.9 551.0 70.1 271.6 21.6EAM-1148-18 788 1880 7.1 0.2255 8.7 0.0320 5.1 0.59 202.9 10.3 206.5 16.3 247.5 163.1 202.9 10.3EAM-1148-19 759 1990 8.2 0.2485 10.3 0.0307 6.3 0.61 195.1 12.1 225.3 20.8 554.1 178.4 195.1 12.1EAM-1148-20 486 5925 2.8 1.2809 4.2 0.1291 3.2 0.76 783.0 23.7 837.2 24.2 984.0 56.4 783.0 23.7EAM-1148-21 1260 5525 5.4 0.2547 7.5 0.0354 5.2 0.69 224.2 11.5 230.4 15.5 293.7 123.9 224.2 11.5EAM-1148-22 988 4890 6.8 0.2334 7.0 0.0344 1.8 0.25 217.7 3.8 213.0 13.5 161.1 158.8 217.7 3.8EAM-1148-23 629 5615 4.2 0.5317 4.8 0.0655 2.4 0.49 408.8 9.3 433.0 17.0 563.8 91.8 408.8 9.3EAM-1148-25 1180 21850 2.6 1.5236 4.6 0.1419 3.8 0.83 855.3 30.6 939.9 28.2 1143.9 50.7 1143.9 50.7

EAM-1148-25A 295 3115 4.8 0.9640 9.1 0.0967 7.7 0.85 595.0 43.7 685.4 45.3 994.5 98.2 595.0 43.7EAM-1148-29 1744 6150 3.0 0.2511 4.9 0.0345 3.9 0.80 218.4 8.4 227.5 10.0 322.9 67.7 218.4 8.4EAM-1148-30 1140 4755 3.3 0.3441 3.7 0.0473 1.8 0.48 297.9 5.2 300.3 9.7 319.2 74.7 297.9 5.2EAM-1148-31 796 3935 6.9 0.3301 11.3 0.0416 8.9 0.79 262.5 23.0 289.6 28.4 514.3 151.4 262.5 23.0EAM-1148-32 1361 6475 4.1 0.6301 6.7 0.0538 5.3 0.79 337.7 17.3 496.2 26.1 1315.1 79.2 337.7 17.3EAM-1148-35 385 1395 6.9 0.3507 7.5 0.0465 3.0 0.40 292.8 8.5 305.2 19.7 401.6 153.6 292.8 8.5EAM-1148-36 919 6055 2.4 0.6395 3.3 0.0703 2.2 0.69 437.8 9.5 502.0 12.9 806.4 49.3 437.8 9.5EAM-1148-38 410 1385 9.8 0.2554 10.0 0.0392 1.8 0.18 247.8 4.4 230.9 20.6 62.3 233.9 247.8 4.4EAM-1148-39 499 9060 3.2 1.6584 5.7 0.1614 4.6 0.82 964.7 41.6 992.8 35.9 1055.2 65.3 1055.2 65.3EAM-1148-41 988 5725 2.7 0.5697 3.7 0.0693 2.5 0.68 431.9 10.5 457.8 13.6 590.1 58.7 431.9 10.5EAM-1148-42 412 2220 3.5 0.7399 4.4 0.0825 2.7 0.61 511.1 13.3 562.3 19.0 775.2 73.2 511.1 13.3EAM-1148-43 1623 21005 1.2 1.1377 4.0 0.1142 3.8 0.95 697.3 25.3 771.4 21.7 992.3 25.1 697.3 25.3EAM-1148-44 476 1050 18.2 0.2512 20.2 0.0341 8.7 0.43 216.0 18.5 227.6 41.1 349.1 414.4 216.0 18.5EAM-1148-45 738 2685 5.8 0.3075 6.5 0.0432 3.0 0.46 272.7 7.9 272.3 15.6 268.9 133.2 272.7 7.9EAM-1148-46 912 2160 5.8 0.2124 9.1 0.0308 7.1 0.78 195.6 13.7 195.6 16.3 195.4 134.2 195.6 13.7EAM-1148-47 528 3010 3.2 0.5044 4.7 0.0622 3.5 0.74 389.2 13.2 414.7 16.1 558.9 69.9 389.2 13.2EAM-1148-51 617 2060 5.8 0.3495 17.6 0.0399 16.6 0.94 252.1 41.1 304.3 46.4 726.9 124.0 252.1 41.1EAM-1148-50 1117 3185 5.0 0.2433 12.0 0.0301 10.9 0.91 191.3 20.5 221.1 23.8 551.8 108.4 191.3 20.5EAM-1148-49 636 1095 12.2 0.2933 12.6 0.0370 3.4 0.27 234.1 7.9 261.2 29.1 511.2 268.2 234.1 7.9EAM-1148-54 550 6030 4.5 0.6955 5.2 0.0839 2.6 0.50 519.3 13.1 536.1 21.8 608.3 98.1 519.3 13.1EAM-1148-56 527 14695 2.0 3.7563 2.5 0.2527 1.5 0.59 1452.6 19.2 1583.5 20.0 1762.5 36.8 1762.5 36.8EAM-1148-57 1216 3420 3.2 0.5491 4.8 0.0659 3.6 0.75 411.4 14.5 444.4 17.3 619.2 68.3 411.4 14.5EAM-1148-58 632 6775 2.7 0.9226 5.9 0.0837 5.2 0.89 518.2 26.0 663.7 28.7 1195.5 53.6 518.2 26.0EAM-1148-60 2414 7740 3.7 0.2605 4.3 0.0362 2.2 0.51 229.1 4.9 235.1 8.9 295.3 83.5 229.1 4.9EAM-1148-61 751 1940 7.0 0.2504 9.1 0.0314 5.8 0.64 199.4 11.3 226.9 18.5 522.4 154.4 199.4 11.3EAM-1148-64 283 7625 2.6 1.5274 4.9 0.1514 4.1 0.85 909.0 34.8 941.5 29.8 1018.3 52.5 909.0 34.8EAM-1148-65 95 860 36.4 0.2781 36.4 0.0420 1.0 0.03 265.3 2.6 249.1 80.6 99.4 887.7 265.3 2.6EAM-1148-66 459 2040 12.1 0.2929 12.3 0.0424 2.3 0.18 267.9 5.9 260.8 28.4 198.1 282.6 267.9 5.9EAM-1148-67 98 1010 43.6 0.3216 43.7 0.0414 2.1 0.05 261.5 5.3 283.1 108.4 466.3 1012.7 261.5 5.3EAM-1148-68 148 4470 4.3 1.3630 4.6 0.1403 1.8 0.38 846.6 14.0 873.2 27.2 941.0 88.0 846.6 14.0EAM-1148-69 234 505 17.7 0.1742 17.8 0.0428 1.5 0.08 269.9 3.9 163.0 26.8 -1206.2 553.4 269.9 3.9EAM-1148-73 948 5190 3.4 0.3255 5.4 0.0451 4.2 0.78 284.7 11.8 286.1 13.5 298.1 77.7 284.7 11.8EAM-1148-74 824 3140 6.9 0.2468 7.7 0.0351 3.5 0.45 222.5 7.6 224.0 15.5 239.5 158.3 222.5 7.6EAM-1148-75 214 900 6.3 0.2683 6.5 0.0333 1.7 0.26 211.3 3.5 241.3 14.0 544.6 137.5 211.3 3.5EAM-1148-76 1379 2490 5.5 0.2909 5.8 0.0252 2.1 0.36 160.3 3.3 259.2 13.4 1287.5 106.4 160.3 3.3EAM-1148-78 284 1535 31.5 0.3135 31.7 0.0425 4.2 0.13 268.5 10.9 276.9 77.1 348.6 727.9 268.5 10.9EAM-1148-79 478 3120 9.7 0.4780 10.1 0.0599 2.9 0.28 374.8 10.4 396.7 33.3 526.6 213.5 374.8 10.4EAM-1148-80 354 1035 13.4 0.1912 15.4 0.0294 7.6 0.49 186.5 14.0 177.6 25.2 61.3 321.1 186.5 14.0EAM1148-2 806 4389 4.6 0.2976 6.6 0.0368 4.7 0.72 233.2 10.8 264.6 15.4 552.4 100.5 233.2 10.8EAM1148-4 1844 5376 1.9 0.3072 2.8 0.0419 2.1 0.74 264.9 5.4 272.0 6.7 334.1 42.6 264.9 5.4EAM1148-5 808 8373 3.9 0.3317 4.0 0.0453 1.0 0.25 285.4 2.8 290.9 10.2 334.6 88.4 285.4 2.8EAM1148-6 1347 4575 5.1 0.2497 7.8 0.0321 5.9 0.76 203.8 11.8 226.4 15.8 468.3 113.2 203.8 11.8EAM1148-7 1937 14619 2.6 0.2903 5.3 0.0399 4.6 0.87 252.5 11.4 258.8 12.1 316.4 58.2 252.5 11.4EAM1148-8 1036 6987 3.6 0.2532 5.5 0.0352 4.2 0.76 223.0 9.2 229.1 11.3 292.3 81.5 223.0 9.2

EAM1148-10A 334 1812 7.8 0.2599 7.9 0.0390 1.0 0.13 246.7 2.4 234.6 16.5 115.3 185.0 246.7 2.4EAM1148-11 634 2802 5.1 0.2912 6.5 0.0405 4.0 0.62 256.2 10.0 259.5 14.8 290.2 116.1 256.2 10.0EAM1148-12 634 6171 4.0 0.2652 4.3 0.0374 1.5 0.35 236.6 3.5 238.8 9.1 261.0 92.0 236.6 3.5EAM1148-13 785 1599 5.7 0.2308 9.9 0.0342 8.1 0.82 216.7 17.2 210.8 18.8 145.7 132.7 216.7 17.2EAM1148-14 525 6324 2.1 0.3838 8.3 0.0502 8.0 0.97 315.6 24.6 329.8 23.3 431.5 47.8 315.6 24.6EAM1148-15 719 2580 4.8 0.2128 5.1 0.0313 1.8 0.35 198.4 3.5 195.9 9.1 166.6 112.1 198.4 3.5

ACCEPTED MANUSCRIPT

EAM1148-16 3219 11709 1.9 0.2772 3.2 0.0400 2.6 0.81 253.1 6.3 248.4 7.0 204.4 43.2 253.1 6.3EAM1148-18 168 2955 4.4 0.7951 5.7 0.0892 3.6 0.63 551.0 18.8 594.0 25.6 762.0 93.8 551.0 18.8

EAM1148-18A 539 4050 4.8 0.6154 8.0 0.0417 6.4 0.80 263.4 16.6 487.0 30.9 1749.5 87.1 1749.5 87.1EAM1148-19 473 1737 5.4 0.3029 5.6 0.0404 1.3 0.23 255.5 3.3 268.7 13.1 385.3 121.4 255.5 3.3EAM1148-20 655 21498 1.2 1.4799 4.7 0.1397 4.6 0.97 842.9 36.0 922.2 28.6 1117.0 23.6 1117.0 23.6

S8-1 260 10040 1.6 0.32693 2.9 0.04295 1.6 0.55 271.1 4.2 287.2 7.2 420.8 53.4 271.1 4.2S8-2 429 16805 2.2 0.36262 24.4 0.04582 1.5 0.06 288.8 4.2 314.2 66.0 506.7 543.0 288.8 4.2S8-3 291 13951 1.6 0.28419 1.6 0.03941 1.2 0.75 249.2 2.9 254.0 3.6 298.3 23.8 249.2 2.9S8-4 264 8985 1.9 0.29055 4.6 0.03973 2.0 0.44 251.2 4.9 259.0 10.5 330.4 93.8 251.2 4.9S8-5 187 32250 2.9 1.69371 2.2 0.16659 2.0 0.89 993.3 18.1 1006.2 14.1 1034.3 20.4 1034.3 20.4S8-6 212 1624 1.0 0.32250 8.1 0.03994 3.4 0.42 252.4 8.4 283.8 20.1 551.0 160.9 252.4 8.4S8-7 611 7188 1.4 0.31670 3.8 0.04330 3.4 0.90 273.3 9.2 279.4 9.3 330.6 37.0 273.3 9.2S8-8 117 9506 0.7 0.35541 6.1 0.04487 4.4 0.73 283.0 12.2 308.8 16.2 508.6 92.3 283.0 12.2S8-9 252 27439 0.7 0.87129 3.9 0.10339 3.7 0.97 634.2 22.6 636.3 18.4 643.5 21.7 634.2 22.6

S8-10 168 5978 0.8 0.50850 5.3 0.06465 4.3 0.82 403.9 17.0 417.4 18.1 493.1 66.4 403.9 17.0S8-11 201 39893 1.1 2.08483 1.8 0.19077 1.5 0.84 1125.5 15.8 1143.8 12.6 1178.6 19.9 1178.6 19.9S8-12 338 20851 1.1 0.28319 2.5 0.03879 1.4 0.57 245.3 3.4 253.2 5.6 326.5 47.0 245.3 3.4S8-13 292 16401 0.8 0.35305 2.9 0.04592 2.2 0.76 289.4 6.2 307.0 7.6 442.8 41.4 289.4 6.2

S8-134 24 4484 0.5 2.28447 5.1 0.19342 3.0 0.58 1139.9 31.2 1207.5 36.2 1330.5 80.6 1330.5 80.6S8-14 114 5144 1.1 0.32807 5.2 0.04199 2.5 0.48 265.2 6.6 288.1 13.1 478.4 101.2 265.2 6.6S8-15 91 4191 1.6 0.74717 2.3 0.09106 1.8 0.78 561.8 9.7 566.6 10.0 585.8 31.4 561.8 9.7S8-16 477 15980 0.5 0.30227 2.9 0.04252 2.0 0.67 268.4 5.2 268.2 6.9 266.1 49.7 268.4 5.2S8-17 568 22472 0.6 0.28673 3.4 0.04020 2.8 0.84 254.1 7.0 256.0 7.6 273.3 42.2 254.1 7.0S8-18 435 2183 1.9 0.37488 7.5 0.04834 2.7 0.36 304.3 8.1 323.3 20.7 462.1 154.5 304.3 8.1S8-19 285 19587 2.9 0.42615 2.6 0.05593 2.3 0.88 350.8 7.8 360.4 7.8 422.6 27.4 350.8 7.8S8-20 195 10476 1.6 0.31090 2.4 0.03989 1.8 0.76 252.2 4.5 274.9 5.7 473.0 34.2 252.2 4.5S8-21 299 9089 1.0 0.29207 3.2 0.03984 2.6 0.80 251.9 6.3 260.2 7.3 335.8 43.3 251.9 6.3S8-22 366 3262 1.4 0.34728 17.0 0.04198 5.7 0.33 265.1 14.7 302.7 44.6 603.5 349.5 265.1 14.7S8-23 1135 26539 1.1 0.26511 8.6 0.03917 2.6 0.30 247.7 6.2 238.8 18.2 151.8 191.7 247.7 6.2S8-24 195 4956 1.2 0.29338 2.8 0.03899 1.4 0.52 246.6 3.5 261.2 6.4 394.8 53.0 246.6 3.5S8-25 158 5974 1.3 0.32458 4.8 0.04386 3.8 0.78 276.7 10.2 285.4 12.0 357.2 67.9 276.7 10.2S8-26 250 7023 2.5 0.34853 3.3 0.04672 1.5 0.44 294.3 4.2 303.6 8.7 375.6 66.7 294.3 4.2S8-27 239 6699 1.6 0.28937 2.0 0.03915 1.0 0.49 247.5 2.4 258.1 4.6 354.7 39.9 247.5 2.4S8-28 180 773 0.7 0.30070 9.6 0.04002 4.1 0.43 253.0 10.3 266.9 22.6 391.4 195.0 253.0 10.3S8-29 540 10973 1.2 0.30327 4.8 0.04158 3.5 0.72 262.6 8.9 269.0 11.3 324.3 75.4 262.6 8.9S8-30 193 23634 0.8 1.27040 2.7 0.12948 2.5 0.93 784.9 18.4 832.6 15.3 962.0 20.7 784.9 18.4S8-31 175 5561 1.8 0.29490 4.4 0.03964 2.4 0.54 250.6 5.9 262.4 10.3 369.3 84.3 250.6 5.9S8-32 157 31876 1.3 10.21201 2.7 0.46624 1.4 0.52 2467.0 28.9 2454.2 25.2 2443.5 39.5 2443.5 39.5S8-33 456 25334 3.5 1.36155 2.3 0.14347 1.3 0.57 864.3 10.5 872.5 13.3 893.6 38.6 864.3 10.5S8-34 776 25220 1.1 0.27951 2.2 0.03994 1.5 0.68 252.5 3.7 250.3 4.9 229.5 37.5 252.5 3.7S8-35 672 16700 1.8 0.32440 3.3 0.04418 2.1 0.64 278.7 5.7 285.3 8.1 339.8 56.8 278.7 5.7S8-36 374 24025 2.6 1.40624 2.7 0.14769 2.0 0.75 888.0 16.8 891.6 16.0 900.4 36.8 888.0 16.8S8-37 577 18962 0.9 0.36014 9.1 0.04934 2.7 0.29 310.5 8.1 312.3 24.6 326.2 198.8 310.5 8.1S8-38 224 31081 1.8 3.02548 2.7 0.23688 1.6 0.60 1370.5 20.1 1414.1 20.6 1480.4 41.0 1480.4 41.0S8-39 310 8563 0.7 0.28135 3.0 0.03907 2.0 0.69 247.1 4.9 251.7 6.6 295.2 49.1 247.1 4.9S8-40 1131 2003 1.9 0.25979 4.0 0.03815 1.1 0.27 241.3 2.5 234.5 8.3 166.5 89.4 241.3 2.5S8-41 280 7320 2.6 0.35247 3.9 0.04749 3.0 0.78 299.1 8.9 306.6 10.3 363.8 54.8 299.1 8.9S8-42 339 4335 0.6 0.29775 1.9 0.04074 1.5 0.82 257.4 3.9 264.6 4.4 329.3 24.1 257.4 3.9S8-43 804 27082 1.0 0.28340 2.3 0.03949 1.8 0.80 249.7 4.4 253.3 5.1 287.7 30.6 249.7 4.4S8-44 97 2847 0.9 0.33037 8.6 0.04070 2.9 0.34 257.2 7.3 289.8 21.7 562.4 177.0 257.2 7.3S8-45 1099 37232 1.5 0.30708 1.7 0.04299 1.3 0.79 271.4 3.5 271.9 4.0 276.7 23.5 271.4 3.5S8-46 345 64801 1.1 2.02018 2.0 0.18767 1.6 0.77 1108.7 16.1 1122.3 13.9 1148.7 25.8 1148.7 25.8S8-47 447 11299 1.2 0.27353 5.4 0.03685 2.1 0.40 233.3 4.9 245.5 11.7 364.2 111.1 233.3 4.9S8-48 377 18960 1.5 0.26353 2.0 0.03706 1.7 0.85 234.6 3.9 237.5 4.2 266.3 23.8 234.6 3.9S8-49 596 92395 8.1 1.66113 2.9 0.16318 2.7 0.94 974.4 24.6 993.8 18.4 1036.8 20.2 1036.8 20.2S8-50 280 14882 1.5 0.38025 27.4 0.04613 2.9 0.11 290.7 8.2 327.2 76.9 595.6 601.8 290.7 8.2S8-51 153 6519 1.0 0.29078 4.5 0.03797 1.8 0.40 240.2 4.2 259.2 10.2 434.0 91.5 240.2 4.2S8-52 407 20066 1.5 0.31833 2.7 0.04234 2.1 0.78 267.3 5.5 280.6 6.7 393.1 38.4 267.3 5.5S8-53 702 38815 0.9 0.31023 2.8 0.04306 2.1 0.73 271.8 5.5 274.4 6.8 296.4 43.9 271.8 5.5S8-54 187 9566 0.5 0.30182 3.6 0.04119 1.8 0.49 260.2 4.6 267.8 8.6 334.9 71.8 260.2 4.6S8-55 62 15063 0.8 2.16270 2.5 0.19343 2.0 0.78 1139.9 20.4 1169.1 17.3 1223.7 30.6 1223.7 30.6S8-56 243 11111 1.0 0.27789 2.9 0.03786 2.5 0.86 239.5 5.9 249.0 6.4 338.9 33.0 239.5 5.9S8-57 303 8248 0.7 0.26886 3.5 0.03742 2.8 0.80 236.9 6.4 241.8 7.5 289.9 47.7 236.9 6.4S8-58 247 8621 0.8 0.27419 3.7 0.03795 2.4 0.64 240.1 5.6 246.0 8.1 302.7 65.1 240.1 5.6S8-59 498 13595 1.0 0.26148 3.8 0.03634 1.8 0.48 230.1 4.1 235.9 8.0 293.2 76.4 230.1 4.1S8-60 346 5553 1.1 0.28225 2.7 0.03861 2.0 0.72 244.2 4.7 252.4 6.1 329.3 42.3 244.2 4.7S8-61 263 13528 0.6 0.29985 4.0 0.03967 3.7 0.94 250.8 9.1 266.3 9.3 404.6 30.9 250.8 9.1S8-62 456 20181 1.7 0.37454 3.6 0.04941 3.4 0.95 310.9 10.4 323.0 10.0 411.3 24.5 310.9 10.4S8-63 358 16855 0.9 0.29409 3.4 0.03935 3.1 0.93 248.8 7.6 261.8 7.8 379.7 28.6 248.8 7.6S8-64 157 8857 0.7 0.30233 6.7 0.03926 5.3 0.79 248.3 12.9 268.2 15.8 446.3 91.3 248.3 12.9S8-65 404 28308 0.9 0.28708 3.5 0.03979 1.5 0.42 251.6 3.7 256.3 8.0 299.5 73.1 251.6 3.7S8-66 222 6814 0.3 0.37109 4.8 0.04959 3.5 0.72 312.0 10.5 320.5 13.3 382.1 75.7 312.0 10.5S8-67 165 5562 0.7 0.39550 7.9 0.05087 4.4 0.55 319.9 13.7 338.4 22.9 467.5 146.5 319.9 13.7S8-68 233 3982 0.8 0.30029 2.8 0.04021 2.2 0.77 254.1 5.5 266.6 6.7 378.0 40.5 254.1 5.5S8-69 303 9637 1.1 0.31024 5.6 0.04083 2.4 0.43 258.0 6.1 274.4 13.5 416.5 113.4 258.0 6.1S8-70 126 1391 0.8 0.34992 5.3 0.04592 1.7 0.33 289.4 4.9 304.7 14.0 422.9 112.0 289.4 4.9S8-71 93 3099 0.7 0.40810 5.6 0.05065 3.2 0.57 318.5 10.0 347.5 16.4 546.3 99.8 318.5 10.0S8-72 97 7582 0.6 0.86427 5.6 0.10390 4.0 0.71 637.2 24.3 632.5 26.4 615.5 84.9 637.2 24.3S8-73 57 2064 1.0 0.46843 7.4 0.05338 6.2 0.84 335.2 20.3 390.1 24.1 730.0 86.3 335.2 20.3S8-74 227 12044 2.0 0.33578 3.3 0.04389 2.4 0.72 276.9 6.4 294.0 8.3 431.6 50.1 276.9 6.4S8-75 425 36679 5.4 2.06209 3.9 0.14508 2.9 0.74 873.4 23.4 1136.3 26.4 1680.3 47.7 1680.3 47.7

S8-75A 226 18645 1.8 0.72357 3.4 0.08531 1.7 0.50 527.8 8.5 552.8 14.4 657.2 62.8 527.8 8.5S8-76 173 25163 1.9 1.85177 2.5 0.17835 2.3 0.92 1058.0 22.8 1064.1 16.8 1076.6 20.2 1076.6 20.2S8-77 117 3694 0.7 0.31121 5.5 0.04146 4.3 0.78 261.9 10.9 275.1 13.2 389.2 76.5 261.9 10.9S8-78 357 10013 1.1 0.30317 4.2 0.04219 2.7 0.64 266.4 7.0 268.9 9.9 290.3 74.1 266.4 7.0S8-79 392 6715 0.4 0.29746 2.7 0.04169 2.3 0.84 263.3 5.9 264.4 6.4 274.2 34.6 263.3 5.9S8-80 257 5859 0.6 0.31339 4.9 0.04280 2.0 0.41 270.2 5.4 276.8 11.9 333.1 101.9 270.2 5.4S8-81 22 4027 1.2 3.11489 3.6 0.24440 2.7 0.75 1409.5 33.6 1436.4 27.4 1476.4 45.0 1476.4 45.0S8-82 280 16542 1.5 0.45621 5.3 0.06167 5.0 0.94 385.8 18.8 381.6 16.9 356.6 40.5 385.8 18.8S8-83 96 2173 0.4 0.40992 4.9 0.05132 3.6 0.74 322.6 11.3 348.8 14.4 527.2 72.2 322.6 11.3S8-84 372 15451 0.7 0.34395 3.6 0.04633 3.0 0.85 292.0 8.7 300.2 9.3 364.3 42.6 292.0 8.7

ACCEPTED MANUSCRIPT

S8-85 86 4042 0.7 0.40552 5.0 0.04836 4.2 0.85 304.4 12.5 345.6 14.5 632.9 56.7 304.4 12.5S8-86 179 6038 1.0 0.35022 5.4 0.04502 2.3 0.43 283.9 6.3 304.9 14.1 469.0 107.3 283.9 6.3S8-87 295 13044 1.0 0.38266 2.9 0.04999 2.3 0.79 314.5 7.0 329.0 8.1 432.9 39.3 314.5 7.0S8-88 248 4693 0.7 0.35994 3.0 0.04804 2.4 0.78 302.5 7.0 312.2 8.1 385.1 42.5 302.5 7.0S8-89 119 12066 0.9 0.61559 9.9 0.07074 6.1 0.62 440.6 26.1 487.1 38.4 712.1 166.0 440.6 26.1

S8-89A 364 9189 0.6 0.30695 2.0 0.04167 1.7 0.82 263.2 4.3 271.8 4.8 346.6 26.0 263.2 4.3S8-90 139 6323 1.0 0.36310 3.2 0.04523 2.1 0.64 285.2 5.7 314.5 8.7 538.1 54.3 285.2 5.7S8-91 483 5247 0.5 0.33208 6.5 0.04366 1.8 0.28 275.5 4.8 291.2 16.4 419.0 138.8 275.5 4.8S8-92 279 5147 0.6 0.36185 6.4 0.04455 3.0 0.47 280.9 8.2 313.6 17.2 563.9 122.8 280.9 8.2S8-93 265 8914 0.8 0.33130 3.7 0.04292 3.0 0.81 270.9 8.0 290.6 9.4 451.8 48.5 270.9 8.0S8-94 353 17350 0.7 0.31778 3.3 0.04278 2.7 0.82 270.0 7.2 280.2 8.1 365.8 42.2 270.0 7.2S8-95 311 22324 0.9 0.74810 2.9 0.09273 1.9 0.68 571.7 10.6 567.1 12.5 548.9 46.2 571.7 10.6S8-96 409 44443 2.7 0.89806 4.0 0.10732 3.5 0.87 657.1 21.6 650.7 19.1 628.3 42.5 657.1 21.6S8-97 561 23791 0.8 0.31991 3.0 0.04429 2.8 0.94 279.4 7.8 281.8 7.5 302.2 23.6 279.4 7.8S8-98 254 10416 0.4 0.31729 4.0 0.04171 2.7 0.66 263.5 6.8 279.8 9.8 419.0 67.1 263.5 6.8S8-99 124 7328 0.5 0.34768 4.1 0.04261 3.5 0.84 269.0 9.2 303.0 10.8 573.7 47.9 269.0 9.2

S8-999 141 5841 1.4 0.48676 7.2 0.06226 5.6 0.78 389.4 21.1 402.7 23.8 479.8 99.6 389.4 21.1S8-101 272 16258 0.6 0.39056 7.1 0.05146 5.5 0.78 323.5 17.4 334.8 20.3 414.1 100.1 323.5 17.4

S8-101A 91 24366 3.0 2.32736 2.9 0.20996 2.2 0.78 1228.6 25.1 1220.7 20.3 1206.6 35.0 1206.6 35.0S8-1100 468 17393 1.1 0.28778 3.4 0.03986 1.6 0.49 252.0 4.1 256.8 7.7 301.3 67.5 252.0 4.1

R14-1 100 1207 1.8 0.11887 13.1 0.01290 4.3 0.33 82.7 3.6 114.0 14.1 831.9 258.1 82.7 3.6R14-1 93 867 1.1 0.11651 9.6 0.01339 3.3 0.34 85.7 2.8 111.9 10.2 712.5 192.5 85.7 2.8R14-2 430 3063 0.8 0.09128 6.2 0.01319 1.7 0.27 84.5 1.4 88.7 5.3 204.0 139.3 84.5 1.4R14-3 169 1339 1.2 0.10817 6.8 0.01318 4.0 0.60 84.4 3.4 104.3 6.7 586.7 117.8 84.4 3.4R14-4 151 2081 1.4 0.11697 7.4 0.01332 2.4 0.33 85.3 2.0 112.3 7.8 731.9 147.4 85.3 2.0R14-5 157 1546 0.9 0.09690 9.2 0.01384 3.1 0.33 88.6 2.7 93.9 8.3 230.8 201.1 88.6 2.7R14-6 192 1461 0.8 0.09161 5.5 0.01330 2.1 0.38 85.2 1.7 89.0 4.7 193.5 118.3 85.2 1.7R14-7 93 733 0.9 0.11079 12.5 0.01325 4.2 0.33 84.9 3.5 106.7 12.7 626.5 255.5 84.9 3.5R14-8 249 1167 0.6 0.09216 6.1 0.01353 2.3 0.38 86.6 2.0 89.5 5.2 167.5 131.4 86.6 2.0R14-9 510 1775 0.4 0.08699 4.3 0.01308 2.9 0.67 83.8 2.4 84.7 3.5 110.3 75.4 83.8 2.4

R14-10 163 7757 5.3 1.36617 6.8 0.12835 6.1 0.90 778.4 44.7 874.5 39.7 1126.4 58.4 778.4 44.7R14-10A 581 7935 1.6 0.30700 2.8 0.04095 2.4 0.85 258.7 6.1 271.9 6.8 386.2 34.1 258.7 6.1R14-11 223 2187 1.6 0.08720 9.2 0.01283 3.5 0.38 82.2 2.8 84.9 7.5 162.4 198.8 82.2 2.8R14-12 146 18800 2.7 3.60389 5.7 0.26539 3.4 0.61 1517.3 46.6 1550.4 45.2 1595.7 84.5 1595.7 84.5R14-13 72 2991 1.5 0.83539 4.5 0.09175 3.3 0.74 565.9 18.1 616.6 20.9 807.6 63.8 565.9 18.1R14-14 3087 7286 3.5 0.08779 11.3 0.01295 3.5 0.31 83.0 2.9 85.4 9.2 155.3 250.8 83.0 2.9R14-15 360 2243 2.5 0.08551 8.5 0.01302 2.0 0.24 83.4 1.7 83.3 6.8 80.9 196.0 83.4 1.7R14-16 2483 1289 0.6 0.09125 9.2 0.01338 3.7 0.41 85.7 3.2 88.7 7.8 170.3 196.4 85.7 3.2R14-17 949 13415 17.1 8.83130 5.5 0.36521 3.0 0.54 2006.8 50.9 2320.7 50.4 2609.7 77.7 2609.7 77.7R14-18 906 7091 7.5 0.08411 5.4 0.01281 2.3 0.43 82.1 1.9 82.0 4.2 80.0 115.5 82.1 1.9R14-19 79 494 2.2 0.09336 16.8 0.01308 7.2 0.43 83.8 6.0 90.6 14.5 275.2 349.3 83.8 6.0R14-20 66 627 2.8 0.11695 15.4 0.01278 5.8 0.37 81.9 4.7 112.3 16.4 818.1 299.7 81.9 4.7R14-22 345 2415 0.5 0.09822 8.5 0.01353 4.5 0.53 86.7 3.9 95.1 7.7 313.1 164.5 86.7 3.9R14-23 87 741 2.4 0.11702 10.6 0.01314 3.5 0.33 84.1 2.9 112.4 11.2 761.8 210.7 84.1 2.9R14-24 219 1885 0.8 0.09618 6.7 0.01423 3.7 0.55 91.1 3.3 93.2 6.0 149.1 131.6 91.1 3.3R14-25 549 3000 1.0 0.08155 6.3 0.01274 3.6 0.57 81.6 2.9 79.6 4.8 19.8 124.3 81.6 2.9R14-26 81 767 8.5 0.89806 5.5 0.10506 3.4 0.61 644.0 20.6 650.7 26.3 674.0 92.3 644.0 20.6R14-27 116 768 1.2 0.60586 7.8 0.07800 3.6 0.46 484.1 16.7 480.9 30.1 465.7 154.8 484.1 16.7R14-28 50 2229 1.8 1.81957 4.6 0.16874 3.3 0.72 1005.2 30.4 1052.5 30.0 1152.1 63.4 1152.1 63.4R14-29 119 524 1.4 0.08257 11.9 0.01279 4.9 0.41 81.9 4.0 80.6 9.2 40.1 260.2 81.9 4.0R14-30 471 9056 0.7 1.96373 4.1 0.17732 1.6 0.39 1052.3 15.7 1103.2 27.7 1204.8 74.5 1204.8 74.5R14-40 77 487 1.6 0.09941 12.8 0.01291 3.7 0.29 82.7 3.0 96.2 11.8 446.4 274.1 82.7 3.0R14-31 106 816 1.5 0.08504 14.8 0.01280 6.0 0.41 82.0 4.9 82.9 11.8 108.0 321.2 82.0 4.9R14-32 79 1215 1.6 0.11993 8.1 0.01311 2.4 0.29 83.9 2.0 115.0 8.9 817.8 163.1 83.9 2.0R14-33 112 588 1.5 0.07915 17.0 0.01278 4.2 0.25 81.9 3.5 77.3 12.6 -60.0 402.9 81.9 3.5R14-34 66 461 1.9 0.09536 13.9 0.01252 3.8 0.27 80.2 3.0 92.5 12.3 421.5 300.2 80.2 3.0R14-35 68 402 2.4 0.10193 15.9 0.01261 4.0 0.25 80.8 3.2 98.6 15.0 552.8 338.1 80.8 3.2R14-36 110 995 1.4 0.11219 14.1 0.01399 6.5 0.46 89.6 5.8 108.0 14.5 535.2 275.4 89.6 5.8R14-37 191 5549 3.4 0.66839 4.2 0.08297 2.8 0.68 513.8 13.9 519.7 16.9 545.8 66.6 513.8 13.9R14-38 75 2165 1.6 1.60159 4.5 0.16130 1.3 0.28 964.0 11.4 970.8 28.3 986.3 88.6 964.0 11.4R14-39 121 732 2.0 0.08442 11.2 0.01299 4.8 0.43 83.2 4.0 82.3 8.8 56.1 241.4 83.2 4.0

All uncertainties are reported at the 1-sigma level, and include only measurement errors. Systematic errors would increase age uncertainties by 1-2%.

U concentration and U/Th are calibrated relative to NIST SRM 610 and are accurate to ~20%.

Common Pb correction is from 204Pb, with composition interpreted from

Stacey and Kramers (1975) and uncertainties of 1.0 for 206Pb/ 204Pb, 0.3 for 207Pb/ 204Pb, and 2.0 for 208Pb/ 204Pb.

U/Pb and 206Pb/ 207Pb fractionation is calibrated relative to fragments of a large Sri Lanka zircon of 564 ± 4 Ma (2-sigma).

U decay constants and composition as follows: 238U = 9.8485 x 10 -10, 235U = 1.55125 x 10 -10, 238U/ 235U = 137.88

ACCEPTED MANUSCRIPT

Sample MC10 MC46 MC62 MC20 MC26Punta Betín Punta Betín Rodadero Concha Concha

Age 82 82 82 82 82Sm 1.6559 4.771823 3.243 2.024 3.118804Nd 4.443279 13.860661 9.645 5.645 9.090256

Sm/Nd 0.372694 0.344271 0.33623639 0.35854739 0.343093147Sm/144Nd 0.225345 0.20816 0.20391392 0.2174159 0.207448

143Nd/144Nd(0) 0.513095 0.513121 0.513094 0.513144 0.513131std err% 0.0017 0.0016 0.0019 0.0019 0.0017

143Nd/144Nd( t) 0.51297415 0.51300937 0.51298465 0.5130274 0.51301975�(Nd)0 8.91467273 9.42185324 8.89516579 9.87051292 9.61692266�Nd(T) 6.43005399 7.28350832 6.8488071 7.55212902 7.49293094

Rb 2.446 7.5278 1.879 0.6296 2.443Sr 69.45049 201.8905 157.7025 111.752 71.831403

Rb/Sr 0.035215 0.037285 0.011917 0.0056334 0.0340187Rb/86Sr 0.101225 0.107171 0.034256 0.016192 0.098575

87Sr/86Sr (0) 0.703868 0.703504 0.703893 0.703133 0.702944std err% 0.0021 0.0014 0.0015 0.0017 0.0022

87Sr/86Sr (T) 0.70375013 0.70337921 0.70385311 0.70311415 0.70282922