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Lithos 104 (2008) 378 – 404
www.elsevier.com/locate/lithos
Caribbean island-arc rifting and back-arc basin development in the Late
Cretaceous: Geochemical, isotopic and geochronological
evidence from Central Hispaniola
J. Escuder Viruete a,⁎, M. Joubert b , P. Urien b , R. Friedman c , D. Weis c ,
T. Ullrich c , A. Pérez-Estaún d
a
c
Instituto Geológico y Minero de España, C. Ríos Rosas 23, 28003 Madrid, Spain
b
BRGM. Av. C. Guillemin. 45060 Orléans, France
Pacific Centre for Isotopic and Geochemical Research, University of British Columbia, 6339 Stores Road Vancouver, Canada BC V6T 1Z4
d
Instituto Ciencias Tierra Jaume Almera-CSIC, Lluís Solé Sabarís s/n, 08028 Barcelona, Spain
Received 7 September 2007; accepted 21 January 2008
Available online 14 February 2008
Abstract
We present new regional petrologic, geochemical, Sr–Nd isotopic, and U–Pb geochronological data on the Turonian–Campanian mafic
igneous rocks of Central Hispaniola that provide important clues on the development of the Caribbean island-arc. Central Hispaniola is made up of
three main tectonic blocks—Jicomé, Jarabacoa and Bonao—that include four broad geochemical groups of Late Cretaceous mafic igneous rocks:
group I, tholeiitic to calc-alkaline basalts and andesites; group II, low-Ti high-Mg andesites and basalts; group III, tholeiitic basalts and gabbros/
dolerites; and group IV, tholeiitic to transitional and alkalic basalts. These igneous rocks show significant differences in time and space, from arclike to non-arc-like characteristics, suggesting that they were derived from different mantle sources. We interpret these groups as the record of
Caribbean arc-rifting and back-arc basin development in the Late Cretaceous. TheN 90 Ma group I volcanic rocks and associated cumulate
complexes preserved in the Jicomé and Jarabacoa blocks represent the Albian to Cenomanian Caribbean island-arc material. The arc rift stage
magmatism in these blocks took place during the deposition of the Restauración Formation from the Turonian–Coniacian transition (~ 90 Ma) to
Santonian/Lower Campanian, particularly in its lower part with extrusion at 90–88 Ma of group II low-Ti, high-Mg andesites/basalts. During this
time or slightly afterwards adakitic rhyolites erupted in the Jarabacoa block. Group III tholeiitic lavas represent the initiation of Coniacian–Lower
Campanian back-arc spreading. In the Bonao block, this stage is represented by back-arc basin-like basalts, gabbros and dolerite/diorite dykes
intruded into the Loma Caribe peridotite, as well as the Peralvillo Sur Formation basalts, capped by tuffs, shales and Campanian cherts. This
dismembered ophiolitic stratigraphy indicates that the Bonao block is a fragment of an ensimatic back-arc basin. In the Jicomé and Jarabacoa
blocks, the mainly Campanian group IV basalts of the Peña Blanca, Siete Cabezas and Pelona–Pico Duarte Formation, represent the subsequent
stage of back-arc spreading and off-axis non-arc-like magmatism, caused by migration of the arc toward the northeast. These basalts have
geochemical affinities with the mantle domain influenced by the Caribbean plume, suggesting that mantle was flowing toward the NE, beneath the
extended Caribbean island-arc, in response to rollback of the subducting proto-Caribbean slab.
© 2008 Elsevier B.V. All rights reserved.
Keywords: Island-arc; Arc rifting; Back-arc basin; Mantle melting; Hispaniola; Caribbean plate
1. Introduction
Back-arc basins are regions of extension in a subduction zone
setting often located between the active and remnant volcanic
⁎ Corresponding author.
E-mail address: [email protected] (J. Escuder Viruete).
0024-4937/$ - see front matter © 2008 Elsevier B.V. All rights reserved.
doi:10.1016/j.lithos.2008.01.003
arc. Modern examples in the Western Pacific, as the Mariana
Trough back-arc basin, form by initial rifting of an active intraoceanic arc and subsequent sea-floor spreading (Karig et al.,
1978; Parson and Hawkins, 1994; Hawkins, 1995; Taylor et al.,
1996; Larter et al., 2003). During back-arc development a
changing style in the petrogenesis of the magmas and nature of
the mantle sources occurs, from those characteristic of arcs to
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379
Fig. 1. (a) Map of the northeastern Caribbean plate margin modified from Mann (1999). Box shows location of the study area. (b) Schematic geological map of Central
Hispaniola. SFZ = Septentrional fault zone; HFZ, Hispaniola fault zone; BGFZ, Bonao–La Guácara fault zone; SJRFZ, San Juan–Restauración fault zone; EPGFZ,
Enriquillo–Plantain Garden fault zone; La Meseta (LMSZ), Río Baiguaque (RBSZ) and Hato Viejo (HVFZ) fault/shear zones. LCB, Loma de Cabrera; LTB, Loma del
Tambor; MB, Macutico; and ACB, Arroyo Caña batholiths. Encircled number show location of U–Pb geochronological samples.
those typical of sea-floor spreading (Stern et al., 1990; Hergt and
Hawkesworth, 1994; Gribble et al., 1996, 1998; Ewart et al.,
1998; Martínez and Taylor, 2002, 2003). Tectonomagmatic
models proposed for this evolution imply a reorganization of
mantle convective regimes beneath evolving back-arc basins,
from downwelling or lateral flow beneath incipient rifts to
upwelling beneath zones of seafloor spreading (Gribble et al.,
1998; Taylor and Martinez, 2003). Intrinsic to these models is
the occurrence, during initial arc rifting, of magmas derived by
high-degree melting of refractory (from previous melting)
peridotite sources by slab-derived H2O-rich fluids, which
typically gave rise to Mg-rich melts such high-magnesian
andesites and boninites (Shervais, 2001; Ishizuka et al., 2006).
Spreading centres in back-arc basins are a likely tectonic
setting for many ophiolites (suprasubduction zone ophiolites;
Pearce et al., 1995a), where the geochemistry of magmas varies
from island-arc tholeiite (IAT), to transitional between IAT and
mid-ocean ridge basalt (MORB) and MORB, especially in mature
back-arc basins (Swinden et al., 1997; Flower and Dylek, 2003:
Beccaluva et al., 2004). Also, a temporal transition from
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magmatism with a subduction-related geochemical and isotopic
signature to magmatism that lacks this signature is apparently
preserved in some ophiolites. This tectonomagmatic relationship
has been interpreted as a record of the rifting of an island-arc and
the subsequent establishment of a back-arc basin in Appalachian
(Swinden et al., 1990, 1997; Bédard et al., 1998; MacLachlan and
Dunning, 1998), Tethyan (Robertson, 2004; Dylek and Flower,
2003) and Cordilleran ophiolites (Dickinson et al., 1996; Metzger
et al., 2002; Harper, 2003; Shervais et al., 2004). Furthermore, the
occurrence of high-Mg mafic volcanic rocks in ophiolites provide
important constraints on their tectonic origin, due to the unusual
conditions needed to produce these subduction-related magmas,
plus possible asthenospheric potential temperatures and significant lithospheric extension requirements (Falloon and Danyushevsky, 2000). In this context, coeval or slightly younger than the
arc/back-arc transition rocks, mafic volcanic sequences of LREEenriched tholeiites of oceanic island affinity are interpreted as part
of the mature back-arc succession (Pouclet et al., 1995;
MacLachlan and Dunning, 1998; Shervais et al., 2004).
In this paper, we present new regional petrologic, geochemical, Sr–Nd isotopic, and U–Pb geochronological data on the
Turonian–Campanian mafic igneous rocks of Central Hispaniola that provide important constraints on the development of
the Caribbean island-arc. We argue that these rocks show
significant differences in time and space, from arc-like to nonarc-like characteristics, suggesting that they were derived from
different mantle sources. We interpret these groups as the record
of Caribbean arc-rifting and back-arc basin development
processes in the Late Cretaceous. The geodynamical implications of this tectonomagmatic evolution are also discussed, in
particular the flow of magma source domains influenced by the
Caribbean mantle plume.
2. Geodynamic setting
2.1. The Caribbean island-arc
The Caribbean island-arc is subdivided into three domains:
(1) the extinct Early Cretaceous to Paleogene Greater Antilles in
the north, including Cuba, Jamaica, Hispaniola, Puerto Rico,
and the Virgin Islands; (2) the northern South America segment,
including Tobago, Margarita, and Colombian/Venezuelan
allochthons in the south; and (3) the volcanically active Lesser
Antilles in the east, which rest on buried remnants of the southeastern extension of the Cretaceous arc. In the Greater Antilles
(Fig. 1), island-arc volcanic rocks are traditionally subdivided
(Donnelly et al., 1990) into a lower primitive island-arc suite
(PIA), consisting predominantly of spilitized tholeiitic basalt
and dacitic–rhyolitic lavas, and an overlying basaltic to
intermediate calc-alkaline suite (CA). PIA lavas typically
have low large-ion lithophile (LILE), rare earth (REE), and
high field strength element (HFSE) abundances, low Th, U, and
radiogenic Pb, and near-horizontal primitive-mantle normalized
REE patterns; younger CA lavas are distinguished from PIA by
elevated incompatible element abundances and variably
enriched REE patterns. Recent studies in the Greater Antilles,
however, have demonstrated that Caribbean island-arc volcan-
ism produced basalt compositions with a broad range of LREE/
HREE compositions, reflecting a wide variation in mantle
sources and proportions of pelagic sediment subducted beneath
the arc during its 80 Ma long eruptive history (c.a. 125 to
45 Ma; Jolly et al., 1998, 2001, 2006; Schellekens, 1998;
Iturralde-Vinent and McPhee, 1999; Kerr et al., 1999; Lewis
et al., 2002; Escuder Viruete et al., 2006b, 2007b; Marchesi
et al., 2006). This persistent Lower Cretaceous to Late Eocene
subduction-related volcanism is well preserved in Central and
Northeastern Puerto Rico (Jolly et al., 2001, 2006), where volcanic rocks vary in composition from predominantly basalts to
rhyolites, and from low-K island-arc tholeiites (Aptian–Early
Albian), to calc-alkaline basalts (Late Albian), and finally to
high-K, incompatible-element-enriched basalts (Cenomanian–
Maastrichtian). Following an eruptive hiatus (Paleocene), volcanism recommenced in the Eocene with renewed eruption of
calc-alkaline basalts in Puerto Rico and the Virgin Islands.
2.2. The Geology of Central Hispaniola
Located on the northern margin of the Caribbean plate, the
tectonic collage of Hispaniola results from the WSW to SWdirected oblique-convergence of the continental margin of the
North American plate with the Greater Antilles island-arc
system, which began in Eocene to Early Miocene and continues
today (Donnelly et al., 1990; Draper et al., 1994; Mann, 1999).
The arc-related rocks are regionally overlain by Upper Eocene
to Holocene siliciclastic and carbonate sedimentary rocks that
post-date island-arc activity, and record the oblique arccontinent collision in the north, as well as the active subduction
in the southern Hispaniola margin (Dolan et al., 1998). Central
Hispaniola is a composite of oceanic derived units bound by the
left-lateral strike-slip Hispaniola (HFZ) and San Juan-Restauración (SJRFZ) fault zones (Fig. 1). Accreted units mainly
include serpentinized Loma Caribe peridotites, MORB-type
gabbros and basalts, Late Jurassic deep-marine sediments,
Cretaceous volcanic units related to Caribbean–Colombian
oceanic plateau (CCOP; Kerr et al., 1997, 2002; Lapierre et al.,
1999; Escuder Viruete et al., 2007a), and Late Cretaceous arcrelated igneous and sedimentary rocks (Lewis et al., 1991,
2002; Escuder Viruete et al., 2004). These units were variably
deformed and metamorphosed to prenhite-pumpellyte, greenschist and amphibolite facies conditions, but the textures of the
protoliths are often preserved. In the Late Campanian–
Maastrichtian, the shallow limestones of the Bois de Lawrence
Formation were deposited on top of the extinct arc.
3. Tectonic blocks in Central Hispaniola
The internal structure of Central Hispaniola is characterized by
several main NNW-SSE to WNW-ESE trending fault zones
(Fig. 1): La Meseta (LMSZ), Río Baiguaque (RBSZ), Hato Viejo
(HVFZ) and Bonao–La Guácara (BGFZ) fault zones. These fault
zones bound three crustal domains or tectonic blocks, namely:
Jicomé, Jarabacoa, and Bonao, characterized by different
Turonian–Campanian volcanic stratigraphies, geochemical composition and physical characteristics of their constituent igneous
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rocks (see below). The Loma de Cabrera, Loma del Tambor,
Macutico and Arroyo Caña gabbro-tonalitic batholiths were intruded syn-to late-kinematically along these shear and fault zones
mainly during the Coniacian–Santonian interval (90–84 Ma;
Escuder Viruete et al., 2006a). Sedimentary basins filled with the
Magua–Tavera Groups and unconformably deposited over these
juxtaposed tectonic blocks, indicates that the main ductile structure of Central Hispaniola was pre-Middle Eocene. Late Cretaceous fault zones were variably reactivated during Upper Eocene–
Oligocene brittle thrusting and Miocene to Recent uplift of the
Cordillera Central (Contreras et al., 2004).
3.1. The Jicomé block
The Jicomé block is bounded to the north by the LMSZ and to
the south by the SJRFZ (Fig. 1). It is composed of aN3 km thick
sequence of arc-related volcanic, subvolcanic and volcanosedimentary rocks of the Tireo Group, and the overlying Peña
Blanca and Pelona–Pico Duarte Formations (Fig. 2). The Tireo
Group includes two main volcanic sequences with different
geochemical characteristics (Escuder Viruete et al., 2007b). The
lower Constanza Formation constitutes an Albian to Turonian
island-arc tholeiitic suite, dominated by submarine vitric–lithic
tuffs and breccias of andesitic to basaltic composition, with minor
interbedded basaltic flows. The upper Restauración Formation is
characterized by a spatial and temporal association of adakites,
high-Mg andesites and basalts, and Nb-enriched basalts, which
collectivelly define a shift in the composition of the subductionrelated magmas. This stratigraphic interval is mainly represented
by dacitic/rhyolitic explosive volcanism of calc-alkaline affinity,
with subaerial to episodic aerial eruptions and emplacement of
sub-volcanic domes (Lewis et al., 1991, 2002). Fossil and U–Pb/
Ar–Ar geochronological data show that the upper sequence began
to accumulate at the Turonian–Coniacian boundary (~89 Ma) and
continued in the Santonian to Lower Campanian. In the SE area of
the Jicomé block, the Tireo Group is intruded by subvolcanic
hornblende-gabbros of uncertain age (La Cana gabbros). The
Peña Blanca Formation is composed of a 150–250 m-thick
succession of aphyric, non-vesicular basaltic flows, with slightly
LREE-enriched tholeiitic composition (Escuder Viruete et al.,
2004). These contain plagioclase and clinopyroxene microphenocrysts and have ophitic/subophitic textures. The basalts of the
Pelona–Pico Duarte Formation are 500 to 1500 m-thick and
unconformably overlie the volcanic rocks of the Tireo Group.
They are aphyric, vesicular and very homogeneous, with a LREEenriched transitional to alkalic composition. The rocks contain
microphenocrysts of olivine, Ti-augite and plagioclase. A Late
Campanian to Maastrichtian 40Ar-39Ar whole-rock age has been
obtained for these basalts (68.4 ± 0.7 Ma; Escuder Viruete et al.,
unpublished).
3.2. The Jarabacoa block
The Jarabacoa block is bounded to the north by the HFZ or
HVFZ and to the south by the LMSZ or BGFZ (Fig. 2). It
comprises the Loma La Monja volcano-plutonic assemblage, the
El Aguacate Chert, the Duarte Complex, and the Restauración
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Formation of the Tireo Group, as well as the metamorphic
equivalents of the LMSZ amphibolites. The Loma La Monja
assemblage is composed of gabbros, dolerites, basalts and pelagic
sediments, which represent a dismembered fragment of the Late
Jurassic proto-Caribbean oceanic crust (Escuder Viruete et al., in
press). The El Aguacate Chert consists of 150-m thick sequence
of ribbon chert with radiolarian microfauna of Oxfordian to
Tithonian age (Montgomery et al., 1994). The Duarte Complex
comprises a ∼3-km thick sequence of picrites and high-Mg
basalts ofN 96 Ma (probably Aptian), chemically related to plumegenerated magmas (Draper et al., 1994) and similar to the more
enriched CCOP lavas (Lapierre et al., 1999, 2000; Escuder
Viruete et al., 2007a). The El Yujo basal Member of the
Restauración Formation consists of ∼25 m of interbedded ribbon
chert, dark shale and fine-grained tuff. This is overlain by dacite/
rhyolite brecciated flows with small volcanogenic sulphide
deposits. The amphibolites of the LMSZ result from ductile
shearing during the 88–74 Ma interval (40Ar/39Ar in hornblende;
Escuder Viruete et al., 2006a) along the SW boundary of the
Jarabacoa block. Mafic protoliths are mainly high-Mg basalts of
the Duarte Complex and basalts with flat to slightly LREEenriched patterns of the Peña Blanca Formation.
A regionally developed suite of distinctive mafic intrusions,
referred as the Los Velazquitos gabbros, were preferentially
emplaced in the NE area of the Jarabacoa block. Earlier workers
assumed that these rocks belonged to the Duarte Complex (Lewis
et al., 1991) or to Late Jurassic oceanic crust (Lapierre et al.,
1999). The larger bodies of the Los Velazquitos gabbros are
laccoliths, up to 3–5 km-long and 1 km-thick, that exhibit a
margin-parallel magmatic foliation and local graded cumulate
layering. The laccoliths are connected by dykes with chilled
margins against the Loma La Monja assemblage host rocks. The
gabbros show a wide range of textures and composition, from
primitive coarse-grained olivine-gabbro, to medium-grained
clinopyroxene-plagioclase gabbro and highly evolved finegrained Fe–Ti-gabbro and diorite.
In the Villa Altagracia area, the Siete Cabezas Formation
unconformably overlies the Duarte Complex directly (Fig. 2). It
is composed of massive and pillowed aphyric basalts, with
minor pyroclastic breccias, vitric tuffs and cherts, intruded by
dolerite dykes (de Lepinay, 1987). Radiolarian content in the
sediments yields a Middle Campanian to Maastrichtian age
(Montgomery and Pessagno, 1999). Sinton et al. (1998) obtained
consistent 40Ar–39Ar ages for whole-rock (69.0 ± 0.7 Ma) and
plagioclase (68.5 ± 0.5 Ma). These ages and the geochemical
characteristics of the lavas (tholeiitic basalts with flat REE
pattern) led Lewis et al. (2002) to attribute this unit to the CCOP.
3.3. The Bonao block
The Late Oligocene to Present displacement of the HFZ
effectively truncates geological features in adjacent Bonao
block to the north (Fig. 1). To the south, the block is bounded by
the Hato Viejo fault zone, which comprises the Loma Caribe
peridotite and the Peralvillo Sur Formation, as well as several
gabbro and dolerite bodies. Due to the fact that the block is
composed of a peridotite basement intruded and/or covered by
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igneous mafic rocks, it has been considered of ophiolitic
character (Lewis et al., 2002), though it lacks of a complete
ophiolite stratigraphy. The Loma Caribe peridotite is mainly
composed of spinel harzburgite, but clinopyroxene-rich harzburgite, dunite, lherzolite and small bodies of podiform
chromitites also occur (Lewis et al., 2006). The peridotites are
typically extensively serpentinized and variably sheared, in
particular toward the upper structural contact. The overlying
rocks consist of hundred-meter-sized bodies of layered gabbro
that pass structurally upward into massive, isotropic gabbro.
Individual dolerite dykes intrude serpentinized peridotites and
gabbroic rocks, showing chilled margins. They become more
abundant upwards in the sequence and to the NE. The Peralvillo
Sur Formation forms a narrow belt immediately northeast of the
Loma Caribe peridotite (Fig. 2). It is composed of a 1500–
2300 m-thick basaltic sequence of massive flows and pillow
lavas that host massive sulfide deposits, and is overlain by
∼ 1000 m of volcaniclastic sediments, tuffaceous mudstone and
cherts with Campanian fauna of radiolaria (de Lepinay, 1987;
Lewis et al., 2002).
3.4. Contemporaneous island-arc related rocks
Caribbean island-arc related rocks of Turonian–Campanian
age occur in the Eastern Cordillera of Hispaniola and on Puerto
Rico. In the Eastern Cordillera (Fig. 2), the deposits are mainly
deep marine and composed of epiclastic graywackes, volcaniclastic mass flows, re-worked carbonates, lavas and tuffs, pelagic
radiolarites and limestones of the Las Guayabas (Cenomanian–
Lower Campanian), Río Chavón (Middle-to Upper Campanian),
and Loma de Anglada (Maastrichtian) Formations. The interbedded volcanic rocks are basalts of the Loma La Vega Member
(Coniacian age; Bourdon, 1985; Lebron and Perfit, 1994).
Recently, García-Senz (2004) interpreted these units as the Late
Cretaceous fore-arc basin deposits of the Caribbean island-arc. In
Puerto Rico, the Central and Northeastern tectonic blocks were
assembled into their actual configuration during mid-Santonian
time, by left-lateral Cerro Mula fault zone (Schellekens, 1998).
The Cenomanian to Maastrichtian stratigraphic sequence is
relevant because it provides insight into lateral correlations
of the Greater Antilles island-arc. Volcanic phases III and IV of
Jolly et al. (1998) include lavas of the Lapa Lava Member of
the Robles Formation (Turonian) and the Perchas Formation
(Cenomanian–Turonian) in the Central block, and Santa Olaya
Formation (Cenomanian–Lower Santonian), the Martín González Formation (mid-Santonian to Lower Campanian) and
Tortugas Andesite (Campanian) members in the Northeastern
block (Jolly et al., 1998, 2001, 2006).
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4. U–Pb geochronology
4.1. U–Pb samples
The main objective of U–Pb geochronology was to correlate
regional data for the onset of the felsic volcanism and gabbroic
plutonism in the Jicomé and Jarabacoa blocks. Analytical
procedures are in the Appendix A and results are reported in
Appendix B. All ages are quoted at the 2σ level of uncertainty.
The selected U–Pb samples were (sample location in Fig. 1) a
rhyolite flow with albite + K-feldspar + quartz phenocrysts
(sample 5JE07), a coarse-grained clinopyroxene + plagioclase
gabbro (sample 5JE79, Los Velazquitos gabbro), and a
subvolcanic medium-grained hornblende-gabbro (sample
6JE29, La Cana gabbro). The rhyolite has an adakitic affinity
and belong to the lowermost stratigraphic levels of the
Restauración Formation in NW Jarabacoa. Separated zircon
grains are clear, pale pink, mostly stubby prims, with aspect
ratios of 1.5–3.5. Four abraded zircon fractions (A, B, D and E)
are all concordant (Fig. 3) and give a weighted 206Pb/238 U age of
89.1 ± 0.9 Ma. This Turonian–Coniacian (geologic time scale
from Gradstein et al., 2004) boundary age is interpreted as the
crystallization age of the sample. The gabbro from Los
Velazquitos intrusive suite has MORB geochemical characteristics with a weak subduction signature. The sample was
collected in the core of a laccolith ~ 100-thick. Extracted zircon
grains are clear, pale pink to colourless, stubby to equant prisms,
with aspet ratios of of ~ 1.5–2.0. Zircon fractions A and C are
slighty younger, showing evidence for minor Pb loss. Fractions
B, D and E are concordant (Fig. 3) and give a weighted
206
Pb/238U age of 89.3 ± 1.6 Ma, which is is interpreted as the
crystallization age of the gabbro. The La Cana gabbro intrudes
the Tireo Group in the SW Villa Altagracia area. This evolved
gabbro (Mg#=28) is rich in Fe–Ti oxides and Nb (21.1 ppm),
and has an E-MORB signature. Zircon grains are turbid, yellow
and brown with some clear sectors, euhedral and prismatic.
Fractions A, B, C and D are concordant and overlapping (Fig. 3)
and give a concordia age (Ludwig, 2003) of 93.35 ± 0.23 Ma,
interpreted as the crystallization age of the rock (Cenomanian–
Turonian boundary).
4.2. Interpretation
The 89.1 ± 0.9 Ma age of the adakitic rhyolite is equivalent to
U–Pb zircon and Ar–Ar hornblende ages, obtained for the
lowermost rhyolite flows of the Restauración Formation in the
Jicomé block (Escuder Viruete et al., 2007b). These results
allow us to establish the onset of the felsic volcanism at the
Fig. 2. Schematic lithostratigraphic columns of the three crustal domains or tectonic blocks in Central Hispaniola, namely Jicomé, Jarabacoa and Bonao, as well as of
the Eastern Cordillera. Encircled numbers show locations of samples for U–Pb geochronology. TG, Tireo Group; RBMb, Río Blanco Member; CFm, Constanza
Formation; DC, Dajabón Chert; CMb; Constanza Member; RFm, Restauración Formation; LCG, La Cana gabbro; PBFM, Peña Blanca Formation; BPPD, basalts of
Pelona–Pico Duarte Formation; TRFm, Trois Rivières Formation; BLFm, Bois de Lawrence Formation; EYMb, El Yujo Member; LVzG, Los Velazquitos gabbros;
SCFm, Siete Cabezas Formation; ATG, Arroyo Toro gabbros; LCGD, Loma Caribe related-gabbros/diorites; PvSFm, Peralvillo Sur Formation; HLFm, Hatillo
Limestone Formation; LGyFm, Las Guayabas Formation; LVgMb, Loma La Vega Member; RHz, Radiolaritic horizon; RChFm, Río Chavón Formation; LAFm,
Loma de Anglada Formation. Ranges of age data in the Jicomé block from Escuder Viruete et al. (2006a, 2007b). Adak, adakites; MB, Macutico batholith; LCB, Loma
de Cabrera batholith; LMSZ, La Meseta shear zone; TBA, tholeitic basalt/andesite suite; HMA, high-Mg andesites; NEBA, Nb-enriched basalts and andesites; BABB,
back-arc basin basalts. Other abbreviations as in Fig. 1.
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Turonian–Coniacian boundary in the Jicomé and Jarabacoa
blocks. Also, this felsic volcanism was contemporaneous with
the widespread emplacement of the hornblende-bearing tonalite
magmas in the Macutico (92–83 Ma; Joubert et al., 2004),
Loma de Cabrera (90–74 Ma; Escuder Viruete et al., 2006a),
and Arroyo Caña (90–84 Ma; Hernáiz Huerta et al., 2000)
batholiths. The age of the gabbro overlaps, within error, the age
of the rhyolite. The mafic intrusive suite of Los Velazquitos
gabbros have a geochemical composition similar to other
gabbro bodies and dolerite dykes intrusive in the Loma Caribe
peridotite, and the volcanic rocks of the Peralvillo Sur
Formation (upper levels dated as Campanian) in the Bonao
block (this study). Thus, geochronological data supports the
synchronicity at ~ 89 Ma of the subduction-related felsic
volcanism, the transitional IAT-MORB type plutonism in the
Jarabacoa block, and the basaltic volcanism in the Bonao block
(see below). La Cana gabbros and basalts of the Peña Blanca
Formation (N74 Ma) have a similar enriched tholeiitic
composition without a subduction signature. The 93 Ma age
of the La Cana gabbros indicates that this non-arc-like
magmatism began in the SE area of the Jicomé block.
5. Geochemistry
5.1. Analytical methods
Samples were powdered in an agate mill, and analysed for
major oxides and trace elements by inductively-coupled plasmamass spectrometry (ICP-MS) analysis with a LiBO2 fusion. This
analytical work was done at ACME Analytical Laboratories Ltd
in Vancouver and results reported in Table 1 (and in Appendix C),
as well as details of analytical accuracy and reproducibility in
Appendix A. For major elements oxides, the detection limits are
in generalb 0.01% (Appendix A). The detection limits for trace
elements are typicallyb 0.1 ppm, except for Ba, Ce, La, Ga and Zr
(0.5 ppm); for some trace elements, they are as low as 0.05 ppm. A
representative subset of samples (Table 2) was also analysed for
Sr and Nd isotopic compositions at the Pacific Centre for Isotopic
and Geochemical Research at the University of British Columbia.
Rb, Sr, Sm and Nd were re-analyzed with a Thermo Finnigan
Element2, a double focussing (i.e., high resolution) Inductively
Coupled Plasma-Mass Spectrometer. Samples were repeatedly
leached with 6N HCl to remove secondary alteration. Separation
of Sr and Nd were separated using the method described in Weis
and Frey (2002). Isotope ratios were measured on a Thermo
Finnigan Triton-TI TIMS in static mode with relay matrix rotation
on single Ta filament and double Re-Ta filament for Sr and Nd
isotopic analyses respectively. Sr and Nd isotopic compositions
were corrected for fractionation using 86Sr/88Sr = 0.1194 and
146
Nd/144Nd = 0.7219. During the course of the analyses, the La
Jolla Nd standard gave an average value of 0.511851 ± 0.000008
(n = 3) and the NBS987 Sr standard gave an average of 0.710241 ±
0.000027 (n = 6). 147Sm/144Nd ratio errors are approximately
~1.5%, or ~0.006 (Weis et al., 2006).
Fig. 3. Concordia diagrams for (1) porphyritic rhyolite (adakite) of the
Restauración Formation (Tireo Group) in the Jarabacoa block (5JE07),
(2) coarse-grained gabbro of the Los Velazquitos intrusive suite in the Jarabacoa
block (5JE79), and (3) La Cana hornblende-gabbro intrusive in the SW area
of the Jicomé block (6JE29). U–Pb procedures and analytical data are in the
Appendix A and B. See text for discussion.
5.2. Chemical changes due to alteration and metamorphism
The analyzed mafic igneous rocks have been variably
altered, deformed and metamorphosed. Consequently, changes
of the bulk-rock chemistry are expected as a consequence of
Author's personal copy
J. Escuder Viruete et al. / Lithos 104 (2008) 378–404
selected mobility of relevant elements during these processes.
Many major (e.g., Si, Na, K, Ca) and trace (e.g., Cs, Rb, Ba, Sr)
elements are easily mobilised by late and/or post-magmatic
fluids and under metamorphism; however, the HFSE (Y, Zr, Hf,
Ti, Nb and Ta), REE, transition elements (V, Cr, Ni and Sc) and
Th, are generally unchanged under a wide range of metamorphic conditions, including seafloor alteration at low to
moderate water/rock ratios (Bienvenu et al., 1990). Therefore,
the geochemical characterization and the discussion on
petrogenesis of the igneous rocks will be based mostly on the
HFSE and REE, as well as the Sm–Nd isotopic system, as it can
be assumed that they were not significantly affected by
alteration or metamorphism at the whole-rock scale.
5.3. Geochemical characteristics of mafic igneous rocks
Inspection of geochemical data for Turonian–Campanian
igneous rocks from throughout Central Hispaniola reveals a
heterogeneous assemblage. In the Nb/Y vs Zr/TiO2 plot (Fig. 4),
volcanic rocks from Restauración Formation and Loma La Vega
Member comprise mainly subalkalic basalt/andesite to rhyodacite, while those from the Peña Blanca, Siete Cabezas and
Pelona–Pico Duarte Formation are dominantly tholeiitic subalkalic, transitional and alkalic basalts. In order to subdivide these
rocks into petrogenetically-meaningful groups, we have utilized
N-MORB normalized multi-element diagrams, which incorporate
the incompatible, inmobile HFSE, REE and Th. These diagrams
reveal the presence and magnitude of positive Th (LFSE) and
negative Nb–Ta (HFSE) anomalies with respect to La (LREE).
Such anomalies in intra-oceanic settings are widely interpreted to
primary reflect supra-subduction zone magmatism, involving
mantle wedge sources that have been contaminated by mass
transfer from the subducting slab (Pearce and Peate, 1995a).
Absence of these anomalies is generally interpreted to reflect
sources that have not been contaminated by subducted material.
The contemporaneous mafic igneous rocks from the different
tectonic blocks can be classified into four broad geochemical
groups: group I, tholeiitic to calc-alkaline island-arc basalts and
andesites; group II, low-Ti, high-Mg andesites and basalts; group
III, tholeiitic back-arc basin basalts and gabbros; and group IV,
tholeiitic to transitional and alkalic oceanic intra-plate basalts. The
geochemical groups of igneous rocks recorded in each tectonic
block will be reviewed below and summarized in Fig. 5.
5.3.1. Group I, tholeiitic to calc-alkaline island-arc basalts and
andesites
The group I is represented by the volcanic rocks of the
Restauración Formation of the Jicomé and Jarabacoa blocks,
and the basalts of the Loma La Vega Member of the Eastern
Cordillera. This group is not represented in the intermediate
Bonao block. As a suite, the basalts and andesites of these units
define a calc-alkaline trend of smoothly decreasing TiO2,
Fe2O3, Cr and Ni with increasing fractionation as monitored by
MgO (TiO2 shown in Fig. 6). TiO2 content range between 0.7
and 1.1 wt.%. La/Yb ratios are consistently elevated (4.7–11.5),
and are similar to those of the contemporaneous volcanic phase
III in both Central and Northeast Puerto Rico (Jolly et al., 1998,
385
2001). In the Fig. 7, the overall trace element characteristics of
the Late Cretaceous Caribbean island-arc is shown by
representative rocks of the Constanza (Albian–Cenomanian)
and Restauración Formation (Turonian–Lower Campanian), the
Loma La Vega Member (Coniacian) and, particularly, the
volcanic phase III of Puerto Rico. All these mafic volcanic rocks
have typical subduction-related trace element features (Pearce
and Parkinson, 1993; Woodhead et al., 1998): LILE are enriched relative to LREE (e.g. Ba/La = 18–80), and both groups
are enriched relative to HFSE (e.g. Ba/Nb = 37–460; La/Nb =
2–8), giving the characteristic Nb–Ta anomalies. In Puerto Rico
(Fig. 7a), the extent of the LREE enrichment ([La/Yb]N = 1.4–8.9)
increases through time from the tholeiitic lavas of the Lapa
Member and Santa Olaya Formation that form the lowermost part
of the shaded area in the figure, through the tholeiitic to calcalkaline lavas of the Lapa Lava Member and Perchas Formation
that form the uppermost part of the shaded area (Jolly et al., 2001).
In the Jicomé block, massive flows and syn-volcanic dykes of
tholeiitic basalts and andesites of the Constanza Formation,
display patterns close to the sub-horizontal followed by N-MORB
([La/Yb]N = 1.1–1.9), though with Nb–Ta negative anomalies,
slight depletion in HREE, and a variable enrichment in the
most subduction-mobile elements such as Th, Sr, Pb and LREE
(Fig. 7c). These subduction-related patterns are similar to those of
the older tholeiitic lavas from Puerto Rico. The basalts of the
Loma La Vega Member have the moderate to strong LREE
enrichment ([La/Yb]N = 6.2–8.3) typical of the younger calcalkaline volcanic rocks from Puerto Rico (Fig. 7b), athough they
show less of a depletion in HREE, probably due to a less depleted
source (or a lower degree of partial melting). Therefore, the mafic
volcanic rocks of group I represent the Late Cretaceous Caribbean
island-arc magmas, where intra-arc variation in the depletion or
enrichment patterns can record dynamic melting process within
the sub-arc mantle wedge (Pearce et al., 1995b). Following Jolly
et al. (2006), the compositional shift from tholeiitic to calcalkaline in the emitted lavas reflects an increase in proportion of
subducted pelagic sediments beneath the arc.
5.3.2. Group II, low-Ti, high-Mg andesites and basalts
The low-Ti, high-Mg andesites and basalts are represented by
mafic flows and tuffs, interbedded with the felsic volcanics of
the Restauración Formation in the Jicomé and Jarabacoa blocks
(Escuder Viruete et al., 2007b). These rocks are characterized by
anomalously high MgO (14.3–4.8 wt.%), Cr (978–226 ppm) and
Ni (186–20 ppm) contents for a basalt–andesite range of SiO2.
The TiO2 content are low and range between 0.2 and 0.6 wt.%
(Fig. 6a), which is lower than group I rocks at a given value
of MgO. The REE patterns of these rocks are similar to the
tholeiitic rocks of group I, having a consistent LREE enrichment
([La/Yb]N = 1.7–4.2) and pronounced negative Nb–Ta anomalies
(Fig. 7d), but the absolute abundances are lower (HREE 0.1–
0.5 × N-MORB) and the negative Zr and Hf anomalies are greater
([Zr/Sm]N = 0.3–1.1; average 0.78). The more primitive samples
can be classified as high-Ca boninites according to the definitions
of Crawford et al. (1989), and the more evolved sample exhibits
intermediate characteristics between the high-Ca and low-Ca
series. However, the alteration or metamorphism could change
Author's personal copy
386
Table 1
Major and trace element data for the diverse groups of igneous rocks in Central Hispaniola
I
I
I
I
I
I
I
I
I
II
II
II
II
II
II
II
Unit
LVg
LVg
LVg
LVg
Cs
Cs
Rs
Rs
Rs
HMA
HMA
HMA
HMA
HMA
HMA
HMA
X (UTM)
Y (UTM)
Rock a
Sample Wt%
SiO2
TiO2
Al2O3
Fe2O3
MgO
CaO
Na2O
K2O
P2O5
MnO
Cr2O3
LOI
SUM
Mg# b
Cr
Co
Ni
V
Rb
Ba
Th
Nb
Ta
La
Ce
Pb
Pr
Sr
Nd
Sm
Zr
Hf
Eu
Gd
Tb
Dy
Y
Ho
Er
Tm
Yb
Lu
466920
2075500
BAS
JG9058
52.41
0.77
19.88
7.3
2.54
6.3
3.98
3.36
0.56
0.13
0.007
2.4
99.64
41
48
15.7
16.2
222
75.3
1668
4.6
3.6
0.2
22.0
44
7.0
5.47
1466.4
22.7
5.6
76.2
2.4
1.77
4.84
0.77
4.0
21.7
0.71
2.04
0.33
1.97
0.32
488233
2079777
AND
JM9062
57.47
0.31
18.06
3.6
1.05
1.91
4.51
7.58
0.19
0.2
0.001
4.8
99.68
37
7
5.2
0.3
67
176.8
280
7.9
6.5
0.3
29.0
54.3
14.5
6.26
223.9
26.1
5.3
139.5
4–0
0.99
5.14
0.78
4.65
30.4
0.98
2.84
0.43
3.15
0.53
479799
2079401
AND
JM9239
60.52
0.28
16.55
3.53
1.57
2.26
5.86
4.19
0.33
0.14
0.002
4.4
99.63
47
14
3.1
0.4
57
89.6
227
7
5.8
0.2
29.4
52.4
9.1
6.28
80.3
25.8
5.6
120.2
3.7
0.89
5.19
0.93
5.48
42.2
1.15
3.72
0.58
4.02
0.65
476745
2080299
AND
JM9274
57.97
0.45
19.09
3.23
1.55
1.09
4.37
8.14
0.08
0.29
0.003
3.3
99.56
49
21
3.1
2.7
65
219.3
99
9.3
8.3
0.4
38.4
69.3
18.0
8.14
232.2
36.2
7.3
155.5
4.5
1.11
6.03
1.06
5.67
37.0
1.17
3.35
0.53
3.70
0.56
–
–
MBAS
MJ9068
55.88
0.74
16.75
8.92
3.11
5.33
5.44
0.38
0.08
0.15
0.005
2.7
99.49
41
34
20.3
b20
313
3.9
125
0.3
0.8
b 0.1
2.9
8.4
0.2
1.28
143.7
7.3
2.1
54.7
2.0
0.75
3.13
0.71
3.64
23.2
0.79
2.46
0.35
2.29
0.37
–
–
PICR
FC9068B
47.89
1.05
16.89
9.04
8.24
11.21
2.82
0.17
0.14
0.15
0.031
2.0
99.63
64
212
45.2
108
193
4.6
75
0.3
2.0
0.1
4.0
11.1
0.4
1.73
270.5
9.9
3.0
84.4
2.4
1.24
3.91
0.74
4.24
26.2
0.88
2.73
0.40
2.48
0.41
341969
2088489
BAS
6JE22A
48.66
0.71
17.09
7.55
7.45
11.09
2.64
0.51
0.1
0.1
0.032
3.7
99.63
66
219
31.6
56
223
8.4
356
0.3
1.6
0.1
3.7
8.8
0.4
1.36
227.9
6.2
2.1
38.6
1.2
0.76
2.5
0.54
3.12
16.8
0.66
1.98
0.29
1.89
0.26
341969
2088489
PICR
6JE22B
46.24
0.8
16.08
7.76
7.37
13.03
2.12
0.26
0.11
0.11
0.047
5.9
99.83
65
322
35.0
104
219
2.4
268
0.5
2.1
0.1
4.8
10.9
0.4
1.67
202.3
8.5
2.3
46.5
1.6
0.83
2.93
0.6
3.21
19.6
0.70
2.19
0.31
1.92
0.30
372366
2083343
AND
6JE110B
57.06
0.43
16.71
4.86
1.81
7.72
4.5
2.22
0.19
0.2
0.008
4.3
100.01
42
55
21.6
14.3
115
48.5
269
4.4
3.9
0.3
22.2
42.3
12.7
5.45
552.4
21.8
4.3
107.3
3.1
0.95
3.96
0.67
3.48
22.9
0.66
2.13
0.33
2.06
0.33
290148
2124049
MAND
MJ9208
53.28
0.17
8
11.79
13.9
8.95
0.71
0.08
0.06
0.26
0.143
2.5
99.84
70
978
61.8
186
181
1.3
18
0.2
0.25
b 0.1
1.2
2.8
b 0.1
0.43
9.7
2.6
0.7
13.1
0.24
0.2
0.82
0.13
0.71
4.1
0.13
0.45
0.07
0.39
0.08
267796
2144784
MBAS
FC9101
53.25
0.31
14.26
10.08
7.68
10.1
2.95
0.12
0.06
0.13
0.068
0.7
99.71
60
465
35.4
24.1
123
1.2
135
0.8
2.2
0.2
3.9
7.0
0.2
0.94
149.5
4.7
1.1
23.7
0.8
0.55
1.66
0.3
2.08
10.5
0.44
1.25
0.15
1.17
0.20
284231
2128860
BAS
MJ9134
52.87
0.26
14.14
10.79
8
8.27
3.2
0.06
0.04
0.17
0.031
1.8
99.63
59
212
47.7
47
220
0.9
144
0.6
1.1
b 0.1
3.0
5.9
0.5
0.74
217.3
3.6
0.9
17.1
0.6
0.37
0.9
0.13
0.79
4.7
0.15
0.51
0.08
0.51
0.08
249913
2145173
MBAS
JE9013
51.85
0.23
13.82
11.44
8.09
11.23
1.53
0.1
0.04
0.17
0.054
1.4
99.95
58
369
45.0
19.6
231
1.7
97
0.05
0.2
b 0.1
1.8
2.9
0.2
0.5
193.3
2.5
0.7
5.5
b 0.5
0.33
0.84
0.15
0.87
5.4
0.19
0.57
0.09
0.61
0.10
250217
2143683
MBAS
JE9012
51.71
0.23
15.21
9.59
6.39
11.75
1.24
0.06
0.02
0.15
0.032
3.4
99.78
57
219
39.0
39.4
179
2.1
55
0.3
0.9
b 0.1
2.2
3.8
b 0.1
0.54
109.9
3.1
0.8
15.1
0.5
0.38
0.84
0.17
1.03
6.5
0.22
0.60
0.10
0.65
0.12
237473
2134044
AND
FC9054
57.39
0.41
13.94
9.25
5.55
4.05
4.32
0.28
0.07
0.13
0.04
4.5
99.93
54
274
34.0
89
207
3.3
270
0.6
2.6
0.1
4.2
9.0
0.6
1.29
263.4
6.0
1.6
38.9
1.4
0.55
1.78
0.31
1.83
10.7
0.37
1.08
0.16
1.01
0.17
256398
2133330
BASAND
FC9058
53.84
0.39
13.53
8.26
4.65
12.01
2.52
0.17
0.05
0.15
0.033
4.3
99.9
53
226
29.7
56
274
1.8
431
0.3
1.7
b0.1
2.4
5.1
2.1
0.68
227.4
3.4
1.0
20.2
0.6
0.45
1.34
0.26
1.52
9.3
0.31
0.91
0.15
0.99
0.15
J. Escuder Viruete et al. / Lithos 104 (2008) 378–404
Group
Author's personal copy
Group
I
I
I
I
I
I
I
I
I
II
II
II
II
II
II
II
Unit
LVg
LVg
LVg
LVg
Cs
Cs
Rs
Rs
Rs
HMA
HMA
HMA
HMA
HMA
HMA
HMA
Table 1 (continued)
III
III
III
III
III
III
III
III
III
IV
IV
IV
IV
IV
IV
IV
Unit
LVz
LVz
LVz
LVz
LVz
LVz
LVz
PvSur
PvSur
LMA
LMA
PB
PB
PB
PB
PB
X (UTM)
Y (UTM)
Rock
Sample Wt%
SiO2
TiO2
Al2O3
Fe2O3
MgO
CaO
Na2O
K2O
P2O5
MnO
Cr2O3
LOI
SUM
Mg# b
Cr
Co
Ni
V
Rb
Ba
Th
Nb
Ta
La
Ce
Pb
Pr
Sr
Nd
Sm
Zr
Hf
Eu
Gd
Tb
Dy
Y
Ho
Er
Tm
Yb
Lu
323799
2127943
GAB
5JE79
49.53
1.07
15.61
10.04
8.38
8.78
2.8
0.61
0.08
0.12
0.036
2.8
99.86
62
246
38.6
28.9
263
8.6
36
b 0.1
1.1
b 0.1
2.3
7.1
0.5
1.12
156
6.6
2.3
56.6
1.7
0.74
3.25
0.6
3.65
24.7
0.89
2.59
0.4
2.43
0.40
323721
2125903
DIQ
5JE63
50.54
0.83
15.6
10.18
7.79
9.24
3.01
0.19
0.06
0.12
0.019
2.3
99.88
60
130
43.3
30.7
259
4.6
27
0.1
0.8
0.08
2.0
5.4
0.4
0.94
145.3
5.3
1.9
41.3
1.2
0.69
2.73
0.48
3.30
21.4
0.75
2.17
0.33
2.18
0.34
323786
2128249
GAB
5JE78
50.27
1.18
15.33
10.33
7.83
9.34
2.82
0.59
0.1
0.16
0.033
2.0
99.98
60
226
37.0
20.0
297
7.5
35
0.05
1.2
b 0.1
2.4
7.5
0.4
1.28
183
7.8
2.7
60.4
2.1
0.94
3.71
0.69
4.21
27.4
0.96
2.81
0.38
2.89
0.43
326569
2124998
GAB
5JE24
51.53
0.89
14.94
9.91
7.35
7.80
3.87
0.26
0.07
0.23
0.021
3.0
99.87
59
144
39.8
34.2
283
3.4
28
0.04
1.0
b 0.1
2.3
6.5
0.3
1.04
218.9
6.2
1.9
49.8
1.6
0.78
3.12
0.52
3.48
22.4
0.80
2.23
0.34
2.26
0.34
323655
2125795
GAB
5JE61
50.11
1.14
15.48
9.73
6.45
11.02
3.07
0.11
0.08
0.13
0.026
2.5
99.85
57
178
33.8
30.0
309
1.1
13
0.1
1.4
0.08
2.5
7.9
0.3
1.38
174.7
7.7
2.7
61.9
1.9
1.05
3.97
0.72
4.44
28.1
0.98
2.83
0.44
2.79
0.45
323701
2125792
GAB
5JE62
52.2
1.38
15.5
11.33
5.61
7.94
3.89
0.38
0.13
0.18
0.02
1.3
99.86
50
137
28.6
24.9
328
3.6
36
0.3
1.7
0.08
3.2
10.1
0.5
1.65
152.5
9.1
3.3
78.6
2.4
1.16
4.47
0.83
5.49
34.5
1.16
3.31
0.52
3.50
0.50
323182
2127980
GAB
5JE76
52.9
1.24
15.33
11.55
4.99
6.56
4.92
0.46
0.11
0.17
0.006
1.6
99.84
46
41
36.9
18.6
355
5.0
54
0.05
1.1
b 0.1
2.8
8.7
0.9
1.40
234.1
7.8
3.0
68.0
2.1
1.06
4.25
0.79
5.03
32.2
1.11
3.14
0.48
3.13
0.51
388479
2071853
BAS
6JE61A
49.76
1.90
14.68
12.46
5.13
9.61
3.45
0.05
0.16
0.19
0.006
2.6
100
45
41
48.0
19
418
0.7
4
b 0.1
2.2
0.3
4.1
12.7
0.3
2.15
167.6
12
3.94
108.0
3.1
1.38
5.30
1.08
6.48
38.8
1.25
4.04
0.62
3.67
0.58
–
–
BASAND
SP-34
53.11
1.09
14.92
9.05
5.52
9.47
4.5
0.1
0.08
0.16
0.007
2.2
100.2
55
90
27.0
40.0
265
0.8
12
0.09
0.9
b 0.1
2.9
8.2
1.5
1.40
69.1
7.8
2.6
74.0
nd
0.97
nd
0.63
4.30
26.0
0.91
2.70
0.40
2.50
0.38
–
–
PICR
5JE1
314473
2132285
DOL
5JE50
48.91
0.92
14.46
10.46
8.51
12.57
1.91
0.07
0.07
0.16
0.038
1.9
99.98
62
260
36.5
41.9
295
b .5
96
b0.1
3.0
0.1
2.5
6.6
0.4
0.98
97.1
5.4
1.8
37.9
1.1
00.70
2.50
0.44
2.92
19.0
0.66
1.88
0.29
1.78
0.30
238330
2139395
BAS
FC9050
52.53
0.66
14.78
10.36
7.04
11.69
1.46
0.08
0.06
0.17
0.044
0.9
99.77
57
301
43.3
49.0
313
0.8
66
0.3
2.8
0.2
2.3
5.5
0.1
0.82
94.7
4.3
1.4
30.9
1.0
0.52
1.61
0.39
2.35
14.6
0.53
1.52
0.24
1.48
0.23
237545
2138655
BASAND
FC9051
53.4
0.80
14.25
10.88
6.45
10.76
1.87
0.11
0.09
0.16
0.071
1.0
99.84
54
486
37.4
72.0
318
0.9
64
0.4
4.0
0.3
3.5
8.9
0.3
1.30
104.6
6.4
1.8
48.1
1.5
0.69
2.51
0.5
3.23
19.5
0.66
2.11
0.29
2.01
0.30
229020
2049072
BAS
GS9807
52.03
0.81
14.24
11.24
6.58
10.61
2.1
0.07
0.09
0.17
0.035
1.8
99.78
54
239
43.2
85
304
b.5
116
0.3
4.3
0.3
3.5
8.4
0.3
1.33
112.3
7.2
2.1
47.5
1.5
0.71
2.50
0.57
3.18
18.4
0.67
1.92
0.32
2.04
0.30
231179
2031656
PICR
SG9780
47.68
1.04
13.49
10.97
8.38
9.78
3.41
0.05
0.08
0.17
0.042
4.5
99.59
60
287
50.3
137
339
2.2
35
0.3
3.9
0.3
2.8
7.5
0.3
1.10
108.3
6.2
2.0
44.4
1.4
0.71
2.80
0.56
2.95
19.2
0.72
2.13
0.32
2.06
0.33
222650
2162500
BAS
PU9020
48.85
3.08
11.71
17.61
5.20
5.61
2.26
0.47
0.29
0.19
0.009
4.5
99.78
37
62
49.2
32.6
686
6.3
312
1.0
13
0.8
10.2
28.1
0.2
4.30
145.8
24.2
7.2
194.8
5.1
2.23
9.13
1.79
10.99
66.9
2.28
6.74
0.95
6.36
1.04
46.53
0.8
13.33
10.98
10.9
10.5
1.96
0.04
0.05
0.17
0.085
4.5
99.85
66
582
49.2
169.7
288
b .5
21
b 0.1
2.8
0.1
2.5
5.9
0.7
0.88
75.2
4.5
1.6
34.3
1.3
0.6
2.01
0.41
2.52
16.8
0.58
1.63
0.25
1.66
0.26
J. Escuder Viruete et al. / Lithos 104 (2008) 378–404
Group
387
Author's personal copy
388
Group
I
Unit
LVg
Table 1 (continued )
I
I
I
I
I
I
I
I
II
II
II
II
II
II
II
LVg
LVg
LVg
Cs
Cs
Rs
Rs
Rs
HMA
HMA
HMA
HMA
HMA
HMA
HMA
Group
IV IV
IV
IV
IV
IV
IV IV
IV
IV
IV IV
IVIV
IV
IV
IV IV
IV
IV
IV
IV
IVIV
IV IV
AdakAdak
IV
Unit
LMSZ
LMSZ
LMSZ
LMSZ
LMSZ
LMSZ
LMSZ
LMSZ
7C 7C
7C 7C
7C7C
7C
7C
BPPD
BPPD
BPPD
BPPD
BPPD
BPPD
BPPD
BPPD
BPPD
BPPD
Rs Rs
LC LC
320155
2122375
AMPH
02J96
47.97
2.22
13.24
17.36
6.81
8.56
2.70
0.24
0.11
0.21
0.005
0.5
99.98
44
63
58.0
89.0
921
2.0
49
0.5
4.0
0.02
4.7
11.4
10.0
1.94
116.0
9.7
nd
71.0
3.2
1.14
4.12
0.8
5.02
27.4
1.13
3.33
0.47
3.20
0.50
265475
2143504
AMPH
FC9103
49.48
0.89
13.94
10.83
9.27
11.98
2.01
0.08
0.08
0.22
0.058
0.8
99.64
63
397
48.5
10.7
289
1.2
35
0.2
2.6
0.2
2.3
6.1
0.5
0.97
87.6
5.8
1.7
38.1
1.3
0.66
2.39
0.43
3.07
17.4
0.66
1.8
0.27
1.95
0.30
265007
2143028
AMPH
FC9102
50.19
1.06
14.19
10.80
7.64
11.47
2.59
0.09
0.07
0.22
0.045
1.3
99.67
58
308
45.1
17.4
332
1.3
52
0.1
3.6
0.3
2.6
7.3
0.3
1.06
146
5.7
1.8
40.2
1.3
0.67
2.66
0.59
3.17
18.9
0.71
2.52
0.28
2.02
0.30
377357
2064710
BAS
2J106
48.9
0.94
14.61
10.3
7.12
12.8
2.33
0.05
0.07
0.16
0.035
2.5
99.82
58
239
41.2
52.2
296
0.6
22
0.22
3.6
0.3
3.13
8.1
0.2
1.20
126.2
6.0
1.88
42.8
1.29
0.76
2.54
0.47
3.10
17.0
0.66
2.01
0.28
1.97
0.29
379322
2063028
BAS
2J107
48.37
0.94
13.66
10.32
8.24
12.82
1.67
0.04
0.07
0.16
0.054
3.6
99.94
61
369
49.9
71.7
291
0.8
11
b 0.1
3.4
0.2
3.1
7.5
0.1
0.99
110.8
5.8
1.8
41.3
1.2
0.84
2.45
0.54
3.03
17.7
0.7
2.01
0.36
2.16
0.31
383078
2060178
BAS
2J108
52.54
1.13
12.79
10.69
6.54
11.99
1.84
0.06
0.11
0.16
0.021
1.9
99.77
55
144
41.5
27.6
358
b0.5
36
0.3
4.5
0.3
4.7
8.9
0.3
1.34
95.3
8.7
2.5
54.2
2.2
0.92
3.32
0.62
3.68
24.7
0.93
2.76
0.38
2.75
0.39
381988
2058441
BASAND
2J109
55.36
1.19
11.44
9.62
5.57
10.91
3.60
0.05
0.10
0.16
0.045
1.9
99.95
53
308
36.4
43.9
283
b 0.5
18
0.16
2.6
0.2
3.5
10.3
0.2
1.64
282.1
8.52
2.57
56.1
1.8
0.91
3.05
0.56
3.65
18.7
0.74
2.12
0.30
1.84
0.276
228250
2128700
PICR
SG9017
47.49
1.43
10.84
10.74
8.49
14.29
0.92
1.06
0.15
0.17
0.185
4.1
99.87
61
1266
46.9
244.0
296
14.4
448
1.9
21.1
1.2
18.1
34.6
1.0
4.27
476.6
19.2
4.4
89.9
2.8
1.40
3.87
0.63
3.53
20.3
0.69
1.89
0.26
1.49
0.26
281579
2105698
BAS
MJ9365
50.19
2.15
13.15
12.79
7.06
11.32
1.77
0.26
0.20
0.18
0.035
0.6
99.71
52
239
49.7
94.0
351
9.7
72
1.5
17.1
1.0
14.4
33.5
0.4
4.19
233.9
19.4
4.9
126.1
3.8
1.63
5.31
0.92
5.39
30.2
0.95
2.72
0.39
2.31
0.34
288902
2105499
BAS
MJ9377
49.07
1.54
13.68
11.46
7.84
11.68
1.94
0.27
0.14
0.17
0.067
1.9
99.76
58
458
48.7
122.0
308
5.2
115
1.1
10.8
0.7
9.3
22.4
0.4
2.94
227.5
13.5
3.6
90.9
2.5
1.23
4.30
0.61
3.74
21.9
0.74
2.14
0.30
1.87
0.25
324105
2118298
DAC
5JE07
67.32
0.36
13.75
6.50
3.22
1.85
1.86
2.06
0.09
0.08
0.022
2.8
99.88
50
157
16.2
24.9
116
40.6
497
1.4
5.5
0.4
12.6
25.8
1.1
2.88
233.5
13.5
2.6
76.1
2.4
0.66
2.40
0.24
1.47
6.3
0.21
0.68
0.11
0.81
0.10
343377
2057240
GAB
6JE29
56.27
1.72
10.86
16.39
3.23
3.98
4.41
0.07
0.65
0.25
0.001
2.0
99.83
28
50
15.2
5.0
13
b 0.5
21
1.7
21.1
1.2
16.4
51.1
0.2
8.52
73.8
43.2
13.0
334.7
9.4
3.49
16.78
3.50
19.24
115.6
4.06
11.61
1.75
10.94
1.68
322374
2127789
MBAS
02J103
49.48
1.59
12.86
14.71
6.15
9.96
2.26
0.26
0.16
0.19
0.02
1.6
99.29
45
143
48.0
26.0
431
1.0
31
0.6
5.0
0.025
3.7
10.9
10.0
1.99
145.0
10.6
2.5
80.0
3.1
1.27
4.91
0.98
6.44
31.3
1.45
4.31
0.66
4.51
0.66
228280
2128700
BAS
SG9016
48.17
3.48
12.8
12.66
7.0
10.05
2.02
0.56
0.30
0.17
0.058
2.5
99.77
52
397
51.6
128.0
419
12.0
177
2.4
29.7
1.9
23
53.9
0.4
6.94
406.7
33.3
7.5
185.5
5.2
2.53
7.34
1.26
6.12
30.8
1.1
2.9
0.41
2.21
0.32
228290
2128700
PICR
SG9015
47.63
3.60
12.87
12.71
7.16
10.54
2.04
0.46
0.32
0.17
0.034
2.0
99.53
53
233
49.3
143.0
404
7.4
196
2.1
25.1
1.4
19.7
47.3
0.3
6.25
346.7
29.9
7.2
178.7
5.1
2.48
7.64
1.28
6.44
31.2
1.11
3.08
0.39
2.29
0.31
Major oxides recalculated to an anhydrous basis. Total Fe as Fe2O3. Geochemical rock groups: group I, tholeiitic to calc-alkaline island-arc basalts and andesites; group II, high-Mg andesites and basalts; group III, tholeiitic back-arc basin basalts and gabbros; and group IV, tholeiitic to
transitional and alkalic oceanic intra-plate basalts. Unit: LVg, Loma La Vega Member; Cs, Constanza Fm, Tireo Group; Rs, Restauración Fm, Tireo Group; HMA, high-Mg andesites/basalts, Tireo Group; LVz, Los Velazquitos gabbros; LC, La Cana gabbros; PvSur, Peralvillo Sur Fm; PB,
Peña Blanca Fm; LMSZ, La Meseta shear zone; 7C, Siete Cabezas Fm; BPPD, Pelona–Pico Duarte Fm.
a
Rock type abbreviations: PICR, picritic basalt/picrite; BAS, basalt; BASAND, andesitic basalt; AND, andesite; DOL, dolerite; GAB, gabbro; DAC, dacite; MBAS, metabasalt; MAND, metaandesite; AMPH. Amphibolite; DIQ, mafic dyke.
b Mg# = 100 * mol MgO/ mol (FeO + MgO); for Fe O /FeO = 0.2.
2
3
J. Escuder Viruete et al. / Lithos 104 (2008) 378–404
X (UTM)
Y (UTM)
Rock
Sample Wt%
SiO2
TiO2
Al2O3
Fe2O3
MgO
CaO
Na2O
K2O
P2O5
MnO
Cr2O3
LOI
SUM
Mg#b
Cr
Co
Ni
V
Rb
Ba
Th
Nb
Ta
La
Ce
Pb
Pr
Sr
Nd
Sm
Zr
Hf
Eu
Gd
Tb
Dy
Y
Ho
Er
Tm
Yb
Lu
IV
Author's personal copy
J. Escuder Viruete et al. / Lithos 104 (2008) 378–404
389
Table 2
Sr–Nd isotope ratios for representative samples of groups III and IV
Group
Rock type
Muestra
Rb
Sr
87Sr/86Sr
(87Sr/86Sr)i
Sm
Nd
143Nd/144Nd
(143Nd/144Nd)i
(ɛNd)i
gabbros suite
gabbros
mafic dyke
gabbros
dolerite
5JE61
5JE63
5JE79
2JE113
1.1
4.6
8.6
3.6
174.7
145.3
156
91.1
0.703526 (7)
0.703960 (7)
0.703964 (9)
0.703764 (9)
0.703503
0.703844
0.703762
0.703617
2.7
1.9
2.3
2.75
7.7
5.3
6.6
8.4
0.513139 (8)
0.513162 (7)
0.513159 (7)
0.513152 (6)
0.513016
0.513036
0.513036
0.513037
9.60
10.00
10.01
10.02
III, Dolerite dyke intrusive en Loma Caribe peridotite (Bayacanes)
BABB
dolerite dyke
6JE66e
0.5
98.8
0.702830 (6)
0.702811
2.31
6.4
0.513122 (6)
0.512995
9.20
IV, Peña Blanca Fm. Jicomé block
E-MORBlavas
E-MORBdolerite
III, Los Velazquitos
BABB
BABB
BABB
BABB
5JE50b
FC9050b
IV, Peña Blanca Fm. Jarabacoa block
E-MORB
lavas
6JE38e
3.8
4.1
122.5
150.9
0.704760 (8)
0.705673 (8)
0.704646
0.705574
2.7
2.1
9.1
6.0
0.512987 (6)
0.513010 (5)
0.512883
0.512887
0.3
41
0.703673 (7)
0.703646
1.1
3.1
0.513020 (6)
0.512895
7.01
7.09
7.25
Calculated initial ratios (i) and ɛNd-values calculated at t = 89 Ma. Number in brackets is the absolute 2σ error in the last decimal places.
ɛNd values are relative to 143Nd/144Nd = 0.512638 and 147Sm/144Nd = 0.1966 for present day CHUR (Jacobsen and Wasserburg, 1980) and lambda 147Sm = 6.54 × 10–
12/year.
the composition of major elements composition. The lower TiO2
and HREE contents (particularly Yb), and negative Zr and Hf
anomalies suggest that the source for group II rocks was more
depleted than for group I tholeiites. Also, the highly magnesian
composition of the group II rocks implies high melting temperatures, a refractory mantle source and relatively rapid transit of the
Fig. 4. Summary of the geochemical groups of mafic igneous rocks recorded
within the different crustal blocks of Central Hispaniola.
magmas through the crust (Falloon and Danyushevsky, 2000;
Yogodzinski et al., 2001).
5.3.3. Group III, tholeiitic back-arc basin basalts and gabbros
The group III is represented by the Los Velazquitos gabbros
and related dolerite dykes in the Jarabacoa block and the basalts
of the Peralvillo Sur Formation in the Bonao block. The Los
Velazquitos gabbros have a restricted range in SiO2 contents,
from 50.2 to 53.8 wt.% (Table 1), for TiO2 contents between 0.8
and 1.5 wt.% (Fig. 6b). In Fig. 4b, the samples cluster mainly in
the subalkaline andesite/basalt field. These gabbros show an
increase of SiO2, Fe2O3T, alkalis, TiO2, Zr and Nb, and a
decrease in Cr and Ni for decreasing MgO. Al2O3 and CaO
increase slightly to reach a maximum at about 7–8 wt.% MgO,
then decrease in the evolved basalts. These trends are tholeiitic
and can be attributed to low-pressure fractionation of olivine
plus Cr-spinel, plagioclase and clinopyroxene, which is
compatible with the observed mineralogy. The gabbros are
more Ti-rich than rocks of groups I and II, defining a mid-Ti
trend in Fig. 6b, but are less titaniferous than most of the
younger group IV basalts. In the Fig. 8, all samples display a flat
HREE pattern ([Sm/Yb]N = 0.9–1.1) and a slight LREE
depletion ([La/Nd]N = 0.6–0.84), characteristic of normal midoceanic ridge basalts (e.g. Natland, 1991). Relative to N-MORB,
however, these rocks have negative Nb–Ta anomalies and
higher abundances of LILE such as Rb, Ba, K, Pb and Sr. Trace
element patterns of the Los Velazquitos gabbros are sub-parallel
to those of the group I samples, although these Caribbean volcanics are more enriched in Th, LILE and LREE. By their
transitional IAT to N-MORB geochemistry and weak subduction-related signature (Fig. 6f), we interpret these gabbros to
form in a back-arc basin setting. The high Zr/Nb ratio of these
rocks suggest a source slightly more depleted than an N-MORB
source.
Volcanic rocks of the Peralvillo Sur Formation also have a
restricted range of SiO2 (48.5–53.4 wt.%) for 7.3–5.0 wt.%
MgO (Table 1) and cluster with the Los Velazquitos gabbros in
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Fig. 5. Nb/Y vs Zr/TiO2 diagram (Winchester and Floyd, 1977) for the geochemical groups of Late Cretaceous igneous rocks in Central Hispaniola defined in the text.
Low-Ti, high-Mg andesites and basalts and felsic volcanics belong to the Restauración Formation in the Jicomé and Jarabacoa blocks.
the subalkaline andesite/basalt field (Fig. 4b). These basalts
show a tholeiitic trend of increasing of SiO2, Fe2O3T,TiO2,
Nb and Zr with decreasing MgO (not all shown in Fig. 6).
The TiO2 content ranges between 0.8 and 2.2 wt.%. These
rocks define a mid-Ti trend with the Los Velazquitos gabbros
in Fig. 6b, but the evolved basalts are slightly more Ti-rich.
The Peralvillo Sur Formation volcanic rocks also display subhorizontal multi-element patterns similar to N-MORB
(Fig. 8c). They are slightly LREE-depleted ([La/Nd]N = 0.7–
0.8) and have flat HREE patterns ([Sm/Yb]N = 1.0–1.5). Moreover, they have small enrichments in the most subductionmobile elements (Rb, Ba, K and Pb), slight depletions in Nb–Ta
with no negative Zr–Hf anomalies ([Zr/Sm]N = 1.0–1.4). All
these characteristics are typical of back-arc basin basalts (e.g.
Hawkins, 1995). A weak subduction signature is indicated
by Nb/Th ratios of 8–16 (Fig. 6f). These features also suggest
that the mantle source for Peralvillo Sur Formation was similar
to both those of the Los Velazquitos gabbros of the Jarabacoa
block and to N-MORB source (i.e. depleted mantle). The source
for group III rocks was therefore more depleted than for both the
arc rocks of group I and, particularly for the high-Mg andesites of
group II.
5.3.4. Group IV, tholeiitic to transitional and alkalic oceanic
intra-plate basalts
Group IV is represented by basalts of the Peña Blanca, Siete
Cabezas and Pelona–Pico Duarte Formation of the Jicomé and
Jarabacoa blocks. Some sampled amphibolites of the LMSZ also
belong to this group (Table 1). The TiO2–MgO variation (Fig. 6b)
shows at least two distinct trends in Ti-contents, where Pelona–
Pico Duarte basalts are more TiO2-rich than Peña Blanca and
Siete Cabezas basalts, as well as LMSZ amphibolites. The basalts
of Peña Blanca Formation have 47.7–53.4 wt.% of SiO2 for
ranges in TiO2 = 0.8–1.1 wt.%, CaO = 9.8–11.7 wt.% and Al2O3 =
13.5–14.8 wt.%. Mg# values of 60–42 indicate that these lavas
are low to moderately fractionated. In Fig. 4b, these basalts
and LMSZ amphibolites cluster between the subalkaline basalt
and andesite basalts fields, but some samples plot close to the
boundary of the alkali basalts field. In the Fig. 9, Peña Blanca
basalts and LMSZ amphibolites have slightly LREE-enriched
([La/Nd]N = 1.0–1.8) and flat HREE ([Sm/Yb]N = 1.0–1.3) patterns, with a positive Nb anomaly and some samples have a
slightly negative Eu and Ti anomalies related to plagioclase and
Fe–Ti oxide frationation. These characteristics are MORB-like
but the rocks have higher concentrations of incompatible elements than group III rocks, indicative of a more enriched mantle
source. Further, they do not have positive Pb, K and Sr spikes, and
negative Nb–Ta anomalies, typical of subduction-related rocks.
All these features, as well as their incompatible element ratios (Zr/
Nb b 15 and La/Sm N 1.5) are characteristics of enriched MORB
(Donnelly et al., 2004). However, some samples have a small
selective enrichment in some fluid-mobile LILE (Rb, Ba, Th and
U), most apparent in the positive Pb spike in the Peña Blanca
Formation of the Jarabacoa block, which probably results from
seafloor alteration. Relatively high-Ti contents, Nb/Th ratios (4–
22; Fig. 6f) and flat-HREE indicate that these magmas were
derived from a relatively enriched spinel mantle source (Donnelly
et al., 2004), which had not been contaminated by a subducting
slab. Probably, these basalts represent a tholeiitic volcanism in
distal areas from the arc or dorsal segments affected by mantle
plume activity (see below).
The basalts of the Siete Cabezas Formation have been described by Sinton et al. (1998) and Lewis et al. (2002). Our
samples have 48.3–55.3 wt.% of SiO2 for ranges in TiO2 =
0.9–1.2 wt.%, CaO=10.2–12.8 wt.% and Al2O3 =11.4–14.6 wt.%,
and cluster in the sub-alkaline basalt field (Fig. 4b). The Mg#
values of 61–53 indicate that these lavas have undergone small
amounts of fractionation. The basalts have slightly LREE-enriched
([La/Nd]N =1.2–1.6) and flat HREE ([Sm/Yb]N =0.9–1.5) multielement patterns, with a positive Nb anomaly. These patterns are
similar to the Peña Blanca basalts, the gabbros and dolerites dredged
from the Beata Ridge (Révillon et al., 2000), and basalts of the
Dumisseau Formation (Sen et al., 1988), suggesting a similar CCOP
plume-related source (Fig. 9d). For similar Mg#, the Siete Cabezas
basalts have higher TiO2, Nb and Zr contents and LREE abundances
than island-arc and HMAvolcanic rocks of previous groups (Fig. 6).
These contents are related to distinct, non-subduction related
enriched sources (see below).
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391
Fig. 6. Plots of (a, b) TiO2 and (c, d) Nb against MgO for the diverse geochemical groups of Late Cretaceous igneous rocks in Central Hispaniola. (e, f) Plots of Nb/Th
against Y to discriminate between arc-like and non-arc-like magmas (Swinden et al., 1997). Major oxides recalculated to an anhydrous basis. In (a), NVTZ, CG and SR
fields are Northern Volcano-Tectonic Zone, Central Graben and Spreading ridge fields of the Mariana Arc-Trough system from Gribble et al. (1998; and references
herein), which are shown for comparison with groups I and II. The labelled arrows show the modelled magmatic evolution accompanying 5% fractionation for a
primitive mafic composition (Escuder Viruete et al., unpublished).
For a restricted range of 47.6–50.2 wt.% SiO2, the Pelona–
Pico Duarte basalts have low CaO (10.1–12.0 wt.%) and Al2O3
(12.8–13.7 wt.%) contents, and high contents in alkalis (2.0–
2.6 wt.%), P2O5 (0.15–0.32 wt.%), TiO2 (1.5–3.6 wt.%), and
Fe2O3 T (10.7–12.8 wt.%). They are all significantly Ti
enriched relative to the older lavas, defining a high-Ti trend in
Fig. 6b. The Mg# values of 58–52 indicate that these lavas have
undergone low to moderate amounts of fractionation. Fig. 4b
shows that these basalts are transitional and alkalic, which is
consistent with their Qtz or Ol normative composition. These
rocks show a typical tholeiitic trend of increasing TiO2, Fe2O3T,
CaO, Al2O3, Zr and Nb, for decreasing MgO (Cr or Ni). These
trends can be attributed to the fractionation of olivine plus Cr-
spinel, clinopyroxene (Ti-augite) and plagioclase, observed as
microphenocrysts in the lavas. The basalts have LREE enriched
([La/Nd]N = 1.5–2.2; Fig. 10) and depleted HREE ([Sm/Yb]N =
2.1–3.7) patterns, with very high Nb contents (11–30 ppm).
The negative Eu and positive Ti anomalies are related to plagioclase and Fe–Ti oxide fractionation/accumulation. These
patterns and other trace element ratios are characteristic of
modern day alkalic oceanic-island basalts (Frey et al., 2002).
The higher TiO2 and [Sm/Yb]N ratios suggest that the mantle
source for these basalts was the most enriched in group IV and
contained garnet. These rocks are interpreted as partial melts of
a plume-related, deep enriched source, which have not been
contaminated by active subduction (Nb/Th N 10 in Fig. 6f).
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Fig. 7. MORB-normalized multi-element plots for samples from: (a) volcanic phase III of Caribbean island-arc of Puerto Rico following nomenclature of Jolly et al.
(1998, 2001); (b) Loma La Vega Member basalts of Eastern Cordillera of Hispaniola; (c) Group I in the Jicomé block; and (d) Group II low-Ti, high-Mg andesites and
basalts of Central Hispaniola (Table 1). MORB-normalizing values are from Sun and McDonough (1989).
5.4. Nd and Sr isotope variations and interpretation
The different geochemical groups identified on the basis of
their trace element contents and ratios also possess characteristic radiogenic isotopic ratios. In the (87Sr/86Sr)i vs (ɛNd)i
diagram of Fig. 11, Caribbean island-arc rocks are represented
by the diagonal field of Loma La Vega basalts of group I
(Lebrón and Perfit, 1994) and Late Cretaceous lavas from
Eastern Puerto Rico block, which is subparallel to a calculated
mixing line between pelagic sediments and a representative arc
basalt (Jolly et al., 2001). The Sr–Nd isotopic data for Loma La
Vega basalts of group I are consistent with the presence of a
subducted sediment component. In Fig. 11, samples of the
groups III and IV are restricted to high (ɛNd)i values between
+ 7.0 and + 10.0 (where i = 89 Ma; Table 2), similar to midocean ridge basalts (Su and Langmuir, 2003). (87Sr/86Sr)i ratios
are highly variable (0.70283 to 0.70557) at very restricted
ranges of (ɛNd)i values between+ 9.6 and+ 10.0 in group III and
between+ 7.0 and+ 7.2 in group IV. This is consistent with
seawater alteration (e.g. Sinton et al., 1998), which shift the
samples from the MORB array to the right, and (87Sr/86Sr)i
ratios therefore are not primary.
The (ɛNd)i values of the group III Los Velazquitos gabbros
and dolerite dykes intrusive in the peridotite are high and
homogeneous, compatible with a source dominated by depleted
mantle, similar to Depleted MORB Mantle composition (DMM,
Su and Langmuir, 2003) without incorporation of pelagic
sediments; the (ɛNd)i values of group IV pillow lavas and finegrained dolerites/gabbros are lower, also compatible with a
depleted source, but more enriched than for group III rocks.
Fig. 11 also show that this enriched source had a similar range
of (ɛNd)i values to the CCOP units, as such the Dumisseau
Formation and 146–150–156 sites of DSDP Leg 15. The high
(ɛNd)i values of basalts of groups III and IV are also inconsistent
with a large pelagic sediment component in the source as in
subduction-related group I. In summary, during the Late
Cretaceous, the source changed from relatively enriched and
affected by a sedimentary component in group I, to depleted and
unaffected by sediments in groups III and IV. With respect to
group III, the source of group IV was slightly more enriched and
similar to those of the Caribbean plume-related units.
6. Discussion
6.1. Mantle and slab contributions
One way to assess the relative contribution of source
composition and subduction component in arc-related igneous
rocks is to plot ratios of incompatible elements, in which the effects
of pooled melting or fractional crystallization/accumulation are
minimized. Following the approach of Pearce and Parkinson
(1993), a Caribbean MORB-OIB array of increasing Zr/Yb, Th/Yb
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Fig. 8. MORB-normalized multi-element plots for group III samples from: (a, b) Los Velazquitos gabbros of the Jarabacoa block; (c) Peralvillo Sur Formation basalts;
and (d) related gabbros and dolerites of the Bonao block (Table 1). Range of group I Caribbean island-arc volcanic rocks from Puerto Rico are also shown for
comparison (data from Jolly et al., 1998, 2001).
and La/Yb with increasing Nb/Yb, is defined by the subductionunmodified lavas from the East Pacific Ridge (Figs. 12 and 13;
data from Su and Langmuir, 2003, PETDB, 2007; and references
herein), considered on the basis of trace element/isotopic
fingerprinting and plate reconstruction models (Pindell et al.,
2005), to belong to the same mantle domain. The Caribbean
MORB-OIB array is completed by samples from the CCOP (Hauff
et al., 2000; Kerr et al., 1997, 1999, 2002; Sinton et al., 1998;
Lapierre et al., 1999, 2000), which generally have higher Nb/Yb
ratios than the global average N-MORB, and suggest the influence
of a Late Cretaceous Caribbean plume in the source enrichment.
This influence means that CCOP samples are enriched relative to
N-MORB, and probably this enriched component decreases in
magnitude with distance from the plume. In the figures, the
Caribbean island-arc trend is represented by the volcanic rocks of
Puerto Rico, which constitute a complete record of subductionrelated volcanism in the area, spanning N70 Ma from Aptian to the
Eocene (data from Jolly et al., 1998, 2001, 2006; Schellekens,
1998). The Caribbean island-arc lavas are displaced from the
MORB-OIB array to much higher concentrations of the subduction-mobile elements Th and La. The inference is that Zr/Yb and
Nb/Yb ratios are little or unaffected by additions of components
during subduction, whereas increases in Th/Yb and La/Yb reflect
addition of slab-derived components (Pearce et al., 1995b).
In the Zr/Yb vs Nb/Yb plot, samples of groups I and II
collectively form a linear trend that passes near average N-MORB
and extend along the Caribbean island-arc trend. Following
Pearce et al. (1995b), the plot shows that for these groups both Zr
and Nb are not present in significant concentrations in the
subduction component. This plot also indicates that samples from
the Peralvillo Sur Formation and the Los Velazquitos gabbros are
generally distinctive from arc-related group I and II in that they
have low Zr/Yb and Nb/Yb ratios (and higher [ɛNd]i). The mantle
source for group III is therefore depleted relative to N-MORB and
interpreted to have experienced previous partial melt extraction,
and hence depletion in incompatible elements. Such depleted
mantle was also unaffected by hotspot and/or plume influences.
Samples from the group IV are variably enriched (higher Nb/Yb)
relative to average N-MORB; amphibolites of the LMSZ and
basalts from the Peña Blanca, Pelona–Pico Duarte and Siete
Cabezas Formation are all significantly enriched and trend to
average E-MORB composition. This, together with their slightly
lower (ɛNd)i values, appears to reflect the influence of the Caribbean plume component in the group IV basalts, which also displace CCOP samples from the MORB-OIB array to higher Nb/Yb
values (opposite to vector B in Fig. 12). In terms of incompatible
element ratios, this enriched component is similar to representative basalts of the Dumisseau Formation and DSDP Leg 15, as
well as gabbros and dolerites from the Beata Ridge (Fig. 12d) all
considered as integral part of the CCOP (Révillon et al., 2000; Sen
et al., 1988; Sinton et al., 1998).
Addition of a variable subduction component to a mantle
source of constant composition results in a vertical trend Fig.
13, as only Th and La are added, while Nb and Yb remain nearly
constant (Pearce et al., 1995a). Arc-related samples of the Loma
La Vega Member, Restauración Formation and group II
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Fig. 9. MORB-normalized multi-element plots for group IV samples from: (a) Peña Blanca Formation basalts of the Jarabacoa block; (b) Peña Blanca Formation
basalts of the Jicomé block; (c) amphibolites of the La Meseta shear zone (LMSZ); and (d) Siete Cabezas Formation basalts of the Villa Altagracia area of the Jarabacoa
block (Table 1). The fields for Caribbean–Colombia oceanic plateau samples from the geographycally nearest Beata Ridge of the Caribbean and the Dumisseau
Formation in Haiti, are shown for comparison (data taken from Révillon et al., 2000; Sen et al., 1988; and Sinton et al., 1998).
particularly follow this vertical trend, whereas group IV
samples of the Peña Blanca, Siete Cabezas and Pelona–Pico
Duarte Formation (plus LMSZ amphibolites) do not. In Fig. 13,
the subduction vector A extends vertically from the Caribbean
MORB-OIB array, with the subduction contribution estimated
by contour lines drawn parallel to the array (Pearce et al.,
1995b). Fig. 13 reveals that the subduction contributions for Th
and La range up to 95 and 80% for Loma La Vega Member,
respectively, being generally smaller for Restauración Forma-
Fig. 10. MORB-normalized multi-element plots for group IV samples from
Pelona–Pico Duarte Formation basalts of the Jicomé block. The fields for
Caribbean–Colombia oceanic plateau samples from the Beata Ridge and the
Dumisseau Formation are also shown for comparison.
tion and group II basalts and andesites. Addition of a subduction
component followed by variable degrees of melting, such as
dynamic melting, gives a trend parallel to but displaced from the
MORB-OIB array (vector C; Pearce et al., 1995b). The trends
Fig. 11. (a) Initial Sr–Nd isotopes ratios for the different geochemical groups of
Late Cretaceous igneous rocks in Central Hispaniola, except group II. Initial
ratios (i) and (ɛNd)i values were at t = 89 Ma. The fields for the Duarte Complex,
Dumisseau Formation, DSDP Leg 15 Sites, Loma La Vega basalts and Late
Cretaceous island-arc lavas from Eastern Puerto Rico, are taken from Lebron
and Perfit (1994), Kerr et al. (1997, 2002), Sen et al. (1988), Jolly et al. (1998,
2001, 2006) and Escuder Viruete et al. (2007a). Depleted MORB mantle
(DMM) Sr–Nd isotopic compositions taken from Su and Langmuir (2003):
DMM average for MORBs far from plumes; D-DMM is 2σ depleted and E-DMM
is 2σ enriched over the average. See text for explanation.
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formed by the group I and II, in particular basalts of the Loma
La Vega Member, run sub-parallel to the regional MORB-OIB
array for Th and La (Fig. 13). Therefore, the arc-related rocks of
groups I and II result from a combination of variable subduction
component added to a variable mantle wedge composition.
Addition of a constant subduction component to a variable
mantle source gives a negative, flat or shallow positive slope as
depleted mantle (with lowest Nb) is affected more than enriched
mantle (Pearce and Peate, 1995a; Leat et al., 2004). In Fig. 13,
basalts of the Peralvillo Sur Formation and Los Velazquitos
gabbros plot close to the Nb/Yb ratio of mean N-MORB or
within the depleted part of the array. Some samples extend to
slightly high contents of Th and La indicating a small subduction input. Therefore, group III samples are interpreted as
being derived from depleted mantle with minor or no subduction
component addition. In contrast, group IV samples from the
Peña Blanca and Siete Cabezas Formation plot in the enriched
part of the MORB array (but more depleted than E-MORB), with
no subduction addition. Basalts of the Pelona–Pico Duarte
Formation plot even more higher Nb/Yb values, and approach
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average OIB composition. In Fig. 13, the Peña Blanca and
Siete Cabezas Formation basalts plot as a tight cluster with a
similar composition to the CCOP, which implies that group IV
samples have a similar enriched Caribbean plume component
and also were unaffected by subduction influences. In summary,
Th/Yb–La/Yb vs Nb/Yb relationships indicate a subduction
component decrease and an enriched Caribbean plume component
increase trough time in the Jicomé, Jarabacoa and Bonao blocks.
6.2. Tectonomagmatic evolution of Central Hispaniola in the
Late Cretaceous
In the models proposed for island-arc rifting and subsequent
back-arc basin development (e.g. the northern Mariana Trough
back-arc basin), systematic changes in magma geochemical and
isotopic compositions reveal a progressive transition from early
arc rift lavas, that are indistinguishable from arc lavas, to later
basalts produced by decompression melting in spreading
centres, as response to a reorganization of mantle convective
regimes (Taylor et al., 1996; Gribble et al., 1998; Martínez and
Fig. 12. Plots of Zr/Yb versus Nb/Yb for the defined geochemical groups of Late Cretaceous igneous rocks in Central Hispaniola. The Caribbean island-arc trend is
represented by the Aptian to Eocene volcanic rocks of Puerto Rico (data from Jolly et al., 1998, 2001, 2006; Schellekens, 1998). A Caribbean MORB-OIB array is
defined by the subduction-unmodified lavas from the East Pacific Ridge (data from Su and Langmuir, 2003, PETDB, 2007; and references therein herein) and
completed by samples from the Late Cretaceous Caribbean–Colombian oceanic plateau (Hauff et al., 2000; Kerr et al., 1997, 2002; Sinton et al., 1998; Lapierre et al.,
1999, 2000). The Caribbean plume enriched component probably increases in magnitude with proximity to the plume. Representative basalts from the Dumisseau
Formation and DSDP Leg 15, as well as gabbros and dolerites from the Beata Ridge, are also shown (data from Révillon et al., 2000; Sen et al., 1988; Sinton et al.,
1998). In the plot, there are three principal types of trend (vector), described in detail by Pearce et al. (1995b): A = variable subduction component; B = variably
enriched mantle wedge; C = variable melt extraction. See text for explanation. N-MORB, E-MORB and OIB values are from Sun and McDonough (1989).
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Taylor, 2002; Taylor and Martinez, 2003). The arc-like to non
arc-like magma evolution recorded in the different blocks of
Central Hispaniola can be related to a similar tectonomagmatic
model, which is conveniently described in terms of four broad
stages illustrated in Fig. 14.
90–89 Ma, hornblende-tonalites with juvenile geochemical
characteristics, inherited either through partial melting of the
lower primitive arc crust by the high heat flow, or through
fractionation of adakitic magmas, also intruded the arc sequences
in Central Hispaniola (Escuder Viruete et al., 2004).
6.2.1. Pre ∼ 90 Ma, Caribbean island-arc
The Tireo Group has been interpreted as record of an
extended episode of volcanic and associated sedimentary
activity in the suprasubduction zone setting of the Caribbean
island-arc (Escuder Viruete et al., 2007b). In the Jicomé block,
the Constanza Formation consists of aN2500-thick sequence of
andesites and basalts that accumulated from the Albian to
Turonian (N 90 Ma). This sequence can be correlated with
contemporaneous tholeiitic basalt–andesite suites elsewhere in
the Greater Antilles (Kerr et al., 1999; Lewis et al., 2002; Jolly
et al., 2006;). The associated gabbroic to ultramafic cumulate
igneous complexes of the Jarabacoa block, which represent the
exhumed roots of the magmatic arc (Escuder Viruete et al.,
2004), also belong to this stage. However, the stratigraphic base
of the sequence is not exposed, and so a considerable section of
pre-Albian geological history is missing.
6.2.3. 90–80 Ma, Trench migration of the Caribbean island-arc
and opening of the Loma Caribe back-arc basin
Immediately following or, as indicates the 5JE79 gabbro age,
temporally overlapping the extrusion of the adakitic dacites/
rhyolites in the Jicomé and Jarabacoa blocks, a long-lived episode
of tholeiitic basaltic volcanism was initiated in Central Hispaniola.
This event is mainly represented by the Peralvillo Sur and the Los
Velazquitos gabbros, as well as mafic dykes and sills intruded in
the serpentinized Loma Caribe peridotite. In modern arcs, this
change from intermediate to acid volcanism, particularly ignimbrites and associated pyroclastic deposits, to eruption of tholeiitic
basalts and dolerite feeder dikes, characterize the transition from
the extensional to the rift stages (Busby et al., 1998; FacklerAdams and Busby, 1998). In the Bonao block, the Peralvillo Sur
Formation and associated igneous rocks, form severalb 2 km-thick
dismembered sheets, structurally adjacent to the Loma Caribe
peridotite. Collectively, the sheets have an ophiolitic stratigraphy
of layered to massive gabbros, dolerites/diorites, flow and pillow
basalts, fine-grained volcaniclastic tuffs, shales and Campanian
cherts. As the Los Velazquitos gabbros of the Jarabacoa block,
these tholeiitic igneous rocks were derived from a depleted mantle
source less affected by a subduction component. Therefore, the
Bonao block is considered to represent a fragment of an ensimatic
Loma Caribe back-arc basin. Microgabbro/diorite and dolerite
dykes intruded in the peridotite are also interpreted to have formed
during this magmatic event. They display a wider range of geochemical types between back-arc basin basalts, N-MORB and
E-MORB, and 6JE66e dolerite has a (ɛNd)i = + 9.2 value indicating derivation from a depleted mantle source.
6.2.2. 90–88 Ma, Caribbean island-arc extension and rifting
In the Jicomé and Jarabacoa blocks, the overlying Restauración Formation is characterized by contemporaneous adakites
(93–83 Ma), high-Mg andesites and basalts and Nb-enriched
basalts, around the Turonian–Coniacian boundary (~90 Ma) to
Santonian/Lower Campanian (Escuder Viruete et al., 2007a,b).
High-Mg mafic lavas were sheared by La Meseta shear zone
(88–74 Ma; Ar–Ar in hornblende) and intruded by syn-kinematic
hornblende-bearing tonalites (87.9 ± 1 Ma; U–Pb in zircon; Joubert
et al., 2004), and their extrusion at 90–88 Ma therefore provides a
critical constraint on our model. In a context of arc magmatism,
Mg-rich melts (high-Mg andesites and boninitic rocks) have been
related to the subduction of a spreading ridge or young oceanic
lithosphere, crustal arc rifting and the initiation of normal back-arc
spreading (e.g. Calmus et al., 2003; McCarron and Smellie, 1998;
Tamura and Tatsumi, 2002; Taylor and Martinez, 2003; Shervais
et al., 2004; Ishizuka et al., 2006).
The extrusion of low-Ti, high-Mg andesites and basalts in
Central Hispaniola is related to an anomalous heat injection at the
base of the Caribbean plate, resulting in elevated geotherms and
promoting hydrous partial melting of subduction-contaminated
depleted mantle sources. To fulfil these thermal and chemical
requirements, the group II rocks are interpreted as result of melting
in an unusual tectonic setting such as arc rifting/back-arc opening
and contemporaneous subduction of young lithosphere, similar to
the high-Mg andesite-adakite association in the Setouchi Belt of
SW Japan (Shimoda et al., 1998; Furukawa and Tatsumi, 1999;
Tatsumi and Hanyu, 2003). The high temperatures required to
produce the Mg-rich melts of group II rocks and the relatively rapid
transit of the magmas through the crust can also be explained by
arc rifting and induced heating (Yogodzinski et al., 2001). From
6.2.4. 80–70 Ma, Arc rollback and sea-floor spreading influenced
by the Caribbean plume
In the Jicomé and Jarabacoa blocks, the basalts of the Peña
Blanca, Siete Cabezas and Pelona–Pico Duarte Formation, as well
as amphibolites of the LMSZ, imply magmatic activity further
removed from the influence of the subducting slab. Group IV
rocks therefore represent the subsequent stage of back-arc
spreading and off-axis magmatism, and are a consequence of
the arc volcanic axis migration toward the northeast by rollback
processes. In the Jicomé block, the highly fragmental nature of the
dacites-rhyolites of the Restauración Formation, with accretionary
lapilli preserved, suggests that volcanic rocks were the product of
Surtseyan-style eruptions and, hence, were erupted in a shallowwater environment. In contrast, the tholeiitic basalts of the
overlying Peña Blanca Formation are dominantly nonvesicular
flow and pillow basalts. These relationships suggest that the Peña
Blanca Formation was deposited in a deep water marine
environment produced by crustal arc extension-related
Fig. 13. Plots of (a to d) Th/Yb and (e to h) La/Yb versus Nb/Yb for the defined geochemical groups of Late Cretaceous igneous rocks in the tectonic blocks of Central
Hispaniola, Caribbean island-arc and Caribbean MORB-OIB array. See text for explanation.
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subsidence. The Siete Cabezas Formation basalts were extruded
over the Duarte Complex directly, through a thinner crust, and
probably they represent a more mature stage of back-arc
development.
The enrichment in Nb/Yb ratio (and in LREE/HREE) relative
to both N-MORB and Caribbean island-arc in the group IV
rocks, suggests that an enriched plume mantle component was
present in the back-arc. These rocks also have significantly
Fig. 14. Schematic tectonomagmatic model for Late Cretaceous Caribbean island-arc rifting and subsequent back-arc basin development, based on the magmatic
evolution recorded in the different blocks of Central Hispaniola. The mantle flow convective regimes beneath rifted arcs and evolving back-arc basins are based on
Gribble et al. (1998) and Taylor and Martinez (2003). (a) The motion of the subducting proto-Caribbean slab drives corner flow advection in the mantle wedge. Water
released by the slab promotes partial melting in the mantle above the solidus (heavy dashed lines), which is progressively depleted of a melt component toward the
volcanic front. Melts rises and gave rise group I tholeiitic basalt/andesite suite and ultramafic/mafic cumulates in the lower arc crust. (b) When Caribbean island-arc
extension commences, the lithosphere rifts near the rheologically weak volcanic front. Hydrated mantle is advected upward into the stretching and thinning lithosphere,
leading to high degrees of melting in the rift phase. As the mantle was previously depleted, the melts are group II low-Ti, high-Mg andesites and basalts. Arc rifting could
be triggered by ridge subduction/collision in the forearc, as suggested the contemporaneous adakitic magmatism (Escuder Viruete et al., 2007b). (c) With increasing
extension a seafloor spreading centre is established near the volcanic front advecting highly hydrated mantle. As consequence, back-arc basin basalt-like group III
magmas result. (d) With continued spreading the extension axis separates from the volcanic front and mantle hydration from the slab decreases. Eventually, the back-arc
spreading system separates sufficiently from the volcanic front that it is not significantly affected by hydration and slab-derived geochemical components. Spreading
centre is now advecting shallow mantle and melts are group IV MORBs, modified by a Caribbean plume enriched component incorporated by lateral flow bellow the
extended arc from the SW. Melts derived from a similar but deeper, Caribbean plume enriched source gave rise to OIB-type off-ridge magmatism in the back-arc area.
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399
Fig. 14 (continued ).
different trace element compositions and generally higher (ɛNd)i
values than the arc-related samples, which rules out derivation of
the magmas by dynamic melting processes from the same
sources. Therefore, these rocks are melts sampling an enriched
component that has migrated into the back-arc basin. Due to the
similar values of petrogenetic tracers (incompatible trace
element ratios and [ɛNd]i values) and geological evidence, the
most likely source of this plume material is the nearby Late
Cretaceous Caribbean mantle plume. The absence of a
Caribbean plume component in the sources of the preCampanian arc-related lavas in Central Hispaniola, suggests
that flow of enriched mantle to the Caribbean arc mantle wedge
region was not fully effective until the establishment of a zone of
mantle upwelling beneath a spreading ridge (i.e. a mantle flow
regime typical of back-arc basins). However, the plume sources
were in detail heterogeneous. Applying the melting models
developed by Kerr et al. (2002) reveals than the Peña Blanca and
Siete Cabezas magmas were derived from a high degree of
melting (10–18%) of a relatively enriched spinel lherzolite
mantle source. Decompression melting in a back-arc spreading
centre, could thus form the E-MORB-type magmas characteristic of the CCOP. The Pelona–Pico Duarte basalts are derived
from a lower melting degree (3–5%) of a more enriched mantle
source containing garnet. This source was therefore deeper and
underwent a lower degree of melting than the source of Peña
Blanca basalts. Spatially restricted to the Jicomé block, the
Campanian Pelona–Pico Duarte transitional and alkaline basalts
probably result from off-axis magmatism in the back-arc area.
6.3. Tectonic implications
The exposed stratigraphic, geochronological and geochemical data indicates that Central Hispaniola is made up of several
different tectonic blocks. These blocks are characterized by
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unique Turonian–Campanian volcanic stratigraphies, indicating
they represent separated, ensialic to ensimatic portions of a
Loma Caribe back-arc basin. Their structural juxtaposition took
place during the closure of the back-arc basin, probably in the
Middle Eocene arc-continent collision. This is consistent with
Caribbean island-arc burial beneath the unconformable Eocene–
Oligocene rocks of the Magua–Tavera Groups and with the
evolution of the Late Eocene–Early Miocene syn-collisional
turbiditic El Mamey Group farther to the northeast (Mann,
1999).
Fig. 15 schematically illustrates the model for the opening of
the Loma Caribe back-arc basin. It is based on the models of
Gribble et al. (1998) for the opening of the northern Mariana
Trough, combined with the more recent plate tectonic
reconstructions for the Caribbean of Pindell et al. (2005). The
tectonic evolution involves (a) intra-arc extension in the
Caribbean island-arc; (b) intra-arc rifting starts forming the
Peralvillo Sur Formation in the Bonao block, while the Jicomé
and Jarabacoa blocks (Restauración Formation) are still in an
extensional phase; and (c) active sea-floor spreading is
propagated sub-parallel to a NNW-SSE trench and associated
a strike-slip fault system (in present coordinates), induced by arc
rollback and the oblique motion of the subducting plate. In (a),
the high-Mg andesites and basalts of the Restauración
Formation constitute the first mafic magmatic products of arc
extension and rifting. In this tectonic setting, collision of a ridge
or other buoyant feature with the subduction-zone forearc at
∼ 90 Ma could give rise arc rifting with subsequent opening of a
back-arc basin, and/or collision of the Cuban forearc with the
Yucatán continental fragment in the Santonian–Campanian could
cause that Caribbean plate to rotate rapidly and trigger back-arc
opening by arc rollback forces, similar (inset in Fig. 15b) the
mechanism proposed by Wallace et al. (2005).
The non-arc-like magmatism of the Peña Blanca and
Pelona–Pico Duarte Formation suggests that the Jicomé block
had drifted away from the active Caribbean arc magmatism by
the Santonian–Campanian. Therefore, this arc crustal block
represent part of the remnant arc crust left behind when the
Caribbean island-arc started to rift and opened into a back-arc
basin during the Santonian–Lower Campanian, while the Loma
La Vega Member basalts and correlatives in Central and Eastern
Puerto Rico, probably represent a younger phase of the
Caribbean arc formed after migration of the volcanic axis
toward the northeast by trench rollback. It is consistent with the
40 km northward migration of the principal volcanic axis in
Central Puerto Rico during Cretaceous subduction described by
Jolly et al. (2001). A similar succession from arc-like to nonarc-like magmatism is also recorded in the Jarabacoa block. The
BABB-like Los Velazquitos gabbros intrude an older oceanic
basement composed of remnants of Late Jurassic crust and/or
Lower Cretaceous Duarte complex, and suggest than the block
represents transitional rather than true back-arc oceanic crust.
401
The tholeiites and associated pelagic sediments of the
Campanian Peralvillo Sur Formation are probably the older
crustal rocks in the Bonao block. The trace element composition
of these basalts incorporate a weak subduction-related component, and are similar to basalts erupted in other mature back-arc
basins. Therefore, the Bonao block represents true back-arc
oceanic crust formed by seafloor spreading. This agrees with the
cr-number [molar Cr/(Cr + Al) = 0.38–0.44] vs mg-number
[molar Mg/(Mg + Fe2+) = 0.59–0.64] of analysed Cr-spinels
from lherzolite bodies of the Loma Caribe peridotite that fall
within the abyssal peridotite array and back-arc basin basalt fields
(Dick and Bullen, 1984). However, a more complex fusion history
has been proposed for this mantle fragment (Lewis et al., 2006)
and further research is in progress. The peridotite is intruded by
undated E-MORB gabbros and dolerites which are derived from
sources unaffected by subduction. Like Peña Blanca, Siete
Cabezas and Pelona–Pico Duarte basalts, their enriched trace
element patterns reflect subsequent back-arc spreading and offaxis magmatism influenced by the Caribbean plume.
7. Conclusions
Based on the Turonian–Campanian volcanic history of the
blocks, geochemical composition and physical characteristics of
their constituent volcanic rocks, the blocks in the Central
Hispaniola are interpreted to represent the remnants of extended
island-arc and oceanic plateau (Jicomé), transitional (Jarabacoa)
and oceanic (Bonao) crust, which formed part of a Loma Caribe
back-arc basin. This back-arc basin formed in response to rifting
of the Caribbean island-arc that started at ~ 90 Ma. The group I
volcanic rocks of the Constanza Formation and associated
cumulate igneous complexes preserved in the Jicomé and
Jarabacoa blocks, represents the previous Albian–Cenomanian
Caribbean island-arc. Theb 90 Ma igneous rocks in Central
Hispaniola provide an evolutionary sequence of arc rifting and
subsequent back-arc basin development. The arc-like magmatism of the rift stage in the Jicomé and Jarabacoa blocks took
place from the Turonian–Coniacian transition to Santonian/
Lower Campanian, particularly in its lower part with extrusion
at 90–88 Ma of group II low-Ti, high-Mg andesites and basalts.
Immediately following or temporally overlapping the extrusion
of adakites in the Jicomé and Jarabacoa blocks, a Coniacian–
Lower Campanian back-arc spreading stage of group III
tholeiitic magmatism was initiated. In the Bonao block, this
event is represented by back-arc basin basalts-like magmas
intruded in the Loma Caribe peridotite, as well as the Peralvillo
Sur Formation basalts capped by tuffs, shales and Campanian
cherts. This dismembered ophiolitic stratigraphy indicates that
the Bonao block is a fragment of an ensimatic back-arc basin. In
the Jicomé and Jarabacoa blocks, the mainly Campanian group
IV basalts of the Peña Blanca, Siete Cabezas and Pelona–Pico
Duarte Formation, imply a magmatic activity further removed
Fig. 15. Schematic model for the Caribbean arc rifting and back-arc basin opening (not to scale) during the Late Cretaceous. Plate tectonic reconstructions for the
Caribbean region are derived from Pindell et al. (2005). See text for explanation. Ji, Jicomé block; Jr, Jarabacoa block; Bo, Bonao block; CC, Central Cuba; EC,
Eastern Cuba; SC, Septentrional Cordillera; EC, Eastern Cordillera; CEP, Central and Eastern Puerto Rico; VSI, Virgin and St. Croix Islands; CH, Central Hispaniola;
SWP, Southwest Puerto Rico; NWH, Northwest Haiti; MF, Muertos forearc; SWH, Southwest Haiti; BR, Beata Ridge; CCOP, Caribbean–Colombian oceanic plateau.
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from the influence of the subducting slab. These rocks therefore
represent the subsequent stage of back-arc spreading and offaxis magmatism, consequence of the arc volcanic axis migration
by rollback processes. The group IV basalts have geochemical
affinities of a mantle domain influenced by the Caribbean
plume. Our data thus suggest that mantle was flowing toward
the NE, beneath the extended Caribbean island-arc, in response
to roll-back of the subducting proto-Caribbean slab.
Acknowledgments
The authors would like to thank John Lewis (George
Washington University) and Gren Draper (Florida International
University) for continued discussions on the igneous rocks in the
Dominican Republic. We are also grateful to Francisco Longo
(Falconbridge Dominicana) and many colleagues of the IGMEBRGM-Inypsa team for help and topic discussions. Dirección
General de Minería of Dominican Government is also thanked by
support. Elisa Dietrich-Sainsaulieu is thanked for her help with
the Sr–Nd isotopic analyses at PCIGR. This work froms part of
the MCYT projects BTE-2002-00326 and CGL2005-02162/BTE
and also received aid from the cartographic project of the
Dominican Republic funded by the SYSMIN Program of the
European Union. Careful reviews from J. Geldmacher, A.C. Kerr
and an anonymous reviewer are much appreciated.
Appendix A. Supplementary data
Supplementary data associated with this article can be found,
in the online version, at doi:10.1016/j.lithos.2008.01.003.
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