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CHAPTER 9
The Paleogene Volcanic Rocks of Cuba and Jamaica: Similarities and Differences
Trevor A. Jackson 1 and Peter W. Scott2
1 Department of Geography and Geology, University of the West Indies, jamaica.
2Camborne School of Mines, University of Exeter, Redruth, Cornwall, England.
ABSTRACT. Paleogene volcanic lava flows and associated pyroclastic rocks are exposed in eastern Cuba in the Sierra Maestra mountain range, and in eastern Jamaica in the Wagwater Belt of the Port Royal mountain range. In Cuba, the volcanic rocks are contained within the El Cobre Group and comprise basalts, basaltic andesites, andesites and dacites, some of which have been hydrothermally altered. In Jamaica, the volcanic rocks are contained in the Wagwater Group; they are distinctly bimodal in composition, with basalts and dacites being the dominant rock types. Metasomatism is also evident in these rocks, which have been altered to spilites and quartz keratophyres. The volcanic rocks of El Cobre show tholeiitic and calcalkaline characteristics that are typical of an island-arc assemblage. In the Wagwater Group only the dacites are arc-related, whereas the basalts are intraplate. The presence of intra-plate basalts in the Paleogene island arc of Jamaica, and their absence in Cuba, implies that the evolution of the arc-back arc system in Cuba was different to that of Jamaica, and is a reflection of the tectonic conditions that existed as the Caribbean Plate migrated ENE.
INTRODUCTION
PALEOGENE VOLCANIC rocks of the Greater Antilles
have been recognized in the islands of Jamaica,
Cuba, Hispaniola, Puerto Rico and the Virgin
Islands. They represent the waning stages of volcanic
arc activity in the Greater Antilles region. A paleo
geographic reconstruction of the Caribbean in the
Early Tertiary by Pindell (1994) shows that Cuba,
Hispaniola, Puerto Rico and the Virgin Islands formed
a separate Greater Antilles arc from Jamaica, which was
a part of the Central America Chortis-Nicaraguan Rise
arc (Fig. 9.1). This chapter compares the petrology of
these two Paleogene arcs using Cuba and Jamaica as
examples.
GEOLOGY AND PETROLOGY
In this study the rock analyses from Cuba were from
samples collected during the IGCP 364 field excur
sion to Santiago de Cuba in November 1996.
Although few in number, the analyses are represen
tative of the suite of volcanic rocks that occurs in the
Sierra Maestra (see Table 9.1). The rock analyses
from the Wagwater Belt were published in Jackson
(1977).
CUBA
The Paleogene volcanic rocks crop out m eastern
Cuba along the southern part of the Oriente Block,
-:! C. ~ Giiii:Joooc hm 11+-!IE T HII!O MliuLI:~o''r.; "'
v
YUCA T AH BASIN KINEMATICS
Cuba
S.U• .s~.-Yuc.at~~n '""'fl'n· ~ &s.n
, Carib NoAm Nlli/Jes ~ _,.
GRENADA BASIN KINEMATICS _,.,.. fwMz~• Carib
SoArn<-J..._G,..,«<o Ura )"" / ~ &sin
Nopp<~s Grenada Terrane
Paleocene ... 59Ma
1. Pindell. I /192
~~~(~~~ is uPlifted as Paoama · d bymLo~&xm •
. : ·Ttf'/QaftdTiJV'IGt:il !wso:m -J
Figure 9.1 Paleogeographic reconstruction of the Caribbean during the Paleocene (from Pindell 1994).
where they unconformably overlie arc-related rocks
of Cretaceous age (lturralde-Vinent 1994). They are
contained within the El Cobre Group, where they
occur in the form of lava flows, pillow lavas and
related volcaniclastics; together with the interbedded
sedimentary rocks, they attain a maximum thick
ness of 6000 m. They make up a major part of the
Sierra Maestra mountain range that trends E-W for
some 250 km.
Throughout the area there is evidence that the
El Cobre volcanics have been subjected to hydrother
mal alteration, with serpentine, chlorite and sericite
being the most common alteration minerals present in
the rocks. In the least altered rocks, plagioclase is the
dominant phenocryst phase, and is associated with
minor amounts of clinopyroxene in the basalts,
basaltic andesites and andesites, and with quartz in the
dacites.
The altered nature of the volcanic rocks is
reflected in their chemistry, particularly among the
more mobile elements such as Na20, K20 and Rb,
and the high LOI values (Table 9.1) . Hence the rocks
are classified using Si02 versus Zr!Ti02 (Fig. 9.2)
rather than Si02 against Na20+K20, known as the
TAS classification ofLeMaitre (1989). The data show
a wide range of Si02 chemistry, and that there are
basalts (45-52% Si02), basaltic andesites (52-57%
Si02), andesites (57-63% Si02), and dacites and rhy
odacites (>63% Si02) present in the El Cobre Group.
The suite of rocks shows tholeiitic and calcalkaline
affinities that are typical of volcanic arc settings (Figs.
9.3 and 9.4). Tholeiitic differentiation trends have also
been detected by Kysar et al. (1998), while calcalkaline
rocks have been reported by Iturralde-Vinent (1996).
Associated with the volcanics are several small
coeval plutons that intrude much of the lower and
TABLE 9.1 Major- and trace-element analyses of volcanic rocks from the El Cobre Group, Sierra Maestra, Cuba.
Major- and trace-elements were analysed using a Philips PW1400 XRF spectometer. Major-e lements were analysed using a Rh tube and trace-ele-ments analysed using a Sc/Mo tube. A fusion bead technique with the sample, a La203 heavy absorber and a eutectic lithium tetraborate/lithium carbonate flux was used for major- and minor-elements. Na and the trace-elements were determined on pressed powder pellets.
wto/o 1 2 3 4 5 6 7
Si02 48.54 48.56 51.08 52.70 57.26 63.8 1 67.18
Ti02 0.84 0.87 0.86 0.89 0.78 0.31 0.32
Al203 18.33 18.27 18.65 16.60 17.48 16.50 17.02
'Fe20 3 11.32 11.03 9.95 11.75 9.06 5.42 4.44
MnO 0.17 0.20 0.17 0.22 0.19 0.15 0.03 MgO 5.18 3.54 5.63 4.22 2.14 1.24 0.63 CaO 5.88 9.00 10.44 4.68 6.40 2.88 3.46 Na20 4.58 2.89 2.39 6.44 4.28 5.75 5.19
K20 0.90 0.39 0.38 0.04 0.64 0.78 0.86
P205 0.11 0.13 0.10 0.13 0.14 0.09 0.16
LOI 5.24 6.23 1.09 3.17 2.88 4.05 1.96
TOTAL 101.17 101.14 100.74 100.60 101.25 100.98 101.39
ppm I -I
;:;;
Ba 530 450 504 226 481 449 441 ""0
~ Rb 15 <5 6 <5 8 13 19
m 0 C1
Sr 245 247 188 129 188 279 270 m z m
y 16 17 16 14 21 10 17 < 0
Zr 71 83 87 90 108 109 106 r"" (1 )o
Nb 4 7 11 7 4 13 10 / h
Ga 19 18 17 16 17 14 13 ;;tJ ,, Zn 121 97 86 138 90 58 21
('1 ;-:
Cu 9 115 85 65 60 - 16 (~
Ni 19 - 36 13 6 19 7 n ( ""
v 219 207 217 278 140 '" - 8 .. . Cr 26 10 79 3 3 3 3 /
(l
Co ')2 4'5 49 - 37 26 22 ~;·
~ )<
'!'rill ~ 111(.11 i11111 IIKidr ~
~'- ---------- 'j
11 0 <=-A.~>o Gfot.ocr. INTO THE THIRD MILLENNIUM
80
Rhyolite
Com/Pan 1...=;-: L.J
70 Rhyodadle-D"'I ; [] ~-------------------
'
----""""·· Trachyte
'fJJ.
0 60 N
Q Andesite
• [] Phonolite
50
Bas-Trach-Neph
40
.001 0.01 0.1 1 10
Zrffi02*0.0001
Figure 9.2 Si02 vs Zr{Ti02 *0.0001 classification of the volcanic and the altered volcanic rocks (after Winchester and Floyd 1977) from El Cobre, Cuba; and Wagwater, Jamaica. Closed squares= El Cobre; open squares= Wagwater.
FeOt
Tholeiitic
•
!w • 0 ~ ; . " ' &C c= ) ~# o '
~~ 8 0°~ ~ ' [[[]
ctJ ct9 ' 0
Calc-Aikalint'
\I
Na20+K20 MgO
Figure 9.3 FMA diagram (after Irvine and Barager 1971) of volcanic and altered volcanic rocks from El Cobre and Wagwater. Closed squares = El Cobre ; open squares = Wagwater.
Ti/100
Zr
Figure. 9.4 Ti/100-Zr-3Y discriminant diagram (after Pearce and Cann 1973) showing plots of mafic volcanic rocks from El Cobre (closed squares) and Wagwater (open squares). A is the field of island-arc tholei itic basalts ; B is the field of MORB, island arc tholeiites and calcalkaline basalts; Cis the field of calcalkaline basalts and D is the field of intra-plate basalts.
middle sections of the El Cobre Group. These plutons
do not display as much alteration as the surrounding
volcanics, and radiometric Kl Ar dates give an early to
middle Eocene age for them (Draper and Barros
1994). These plutons range in composition from
granitoid to dioritoid, and from our study show cal
calkaline and tholeiitic properties.
JAMAICA
In Jamaica, Paleogene volcanic rocks occur m the
Wagwater Belt, although the upper part of the
Summerfield Formation in central Jamaica may be
Paleocene (Ahmad et al. 1988). The Wagwater Belt
is a fault-bounded structural unit that trends
NW-SE and within which approximately 7000 m
of Paleogene volcanic and sedimentary rocks are
contained, referred to as the Wagwater Group
(Green 1977).
The volcanic rocks of the Wagwater Group
show similar field characteristics to the volcanics of El
THE PALEOGENE VOLCANIC ROCKS OF CuBA A'D j ..._, •• ~ ; ;:::~ 1.:
Cobre, in that they occur as lava flows, pillow lavas,
dikes and volcaniclastic rocks. However, unlike the El
Cobre suite, where there is a unimodal distribution of
rock type in which the majority of rocks are basaltic
andesite in composition (Kysar et al. 1998), the vol
canic rocks of the Wagwater Group are distinctly
bimodal in composition, with basalt and dacite being
the dominant rock types Qackson and Smith 1979).
Volcanic rocks of basaltic andesite and andesite com
position are rare. The chemistry of the volcanic rocks
indicates that the basalts are tholeiitic and that the
dacites are calcalkaline (Fig. 9.3).
The two essential minerals in the basalts are
clinopyroxene and plagioclase, with a minor amount
of olivine, whereas the dacites are dominated by pla
gioclase phenocryts with lesser amounts of quartz and
hornblende. As at El Cobre, hydrothermal alteration
has affected the original mineralogy and converted
them to spilites and quartz keratophyres Qackson and
Smith 1978).
Only one small plutonic stock has been reported
in the Wagwater Belt. Isaacs and Jackson (1987)
described a small microgranodiorite body that intrudes
the silicic volcanics in the central part of the Wagwater
Belt. The granodiorite is hydrothermally altered and is
associated with porphyry copper deposits.
COMPARISON
Paleogene volcanic rocks of the El Cobre Group and
the Wagwater Group unconformably overlie Upper
Cretaceous rocks. The Cretaceous geology of the
islands indicates that both were once part of an evolv
ing volcanic arc in which Primative Island Arc (PIA)
volcanism in the Early Cretaceous gave way to calcalka
line volcanism in the Late Cretaceous, with Cuba also
containing Late Cretaceous shoshonites (Donnelly et
al. 1990). On both islands there is a very noticeable
change from a Cretaceous high-K volcanic arc suite to
a Paleogene low- to medium-K volcanic arc suite (Fig.
9.5). In Cuba, high-K calcalkaline and shoshonitic vol
canics have been identified in the Late Cretaceous rocks
of Camaguey (Diaz de Villavilla et al. 1998), while in
m1m~· C II~: Uiilllmi:Dt 'lll!llf1ili!iiiiii!II• MII:JI!iiE!OjiNIILJI!UO
TABLE 9.2 ~~ ;;ma ,~~ o" ma'lc volcanic rocks from the Wagwater Group (Jamaica) and the El Cobre Group (Cuba).
wt% 1 2
Si02 47.51 ± 3.40 49.39 ± 1.46 Ti02 2.46 ± 0.61 0.86 ± 0.02
Al203 14.81 ± 1.21 18.42 ± 0.21
Fe20 3 1.47 ± 1.21 1.61 ± 0.11 FeO 8.35 ± 2.35 9.15 ± 0.61 MnO 0.12 ± 0.05 0.18 ± 0.02 MgO 6.77 ± 2.65 4.78 ± 1.10 CaO 7.17 ± 2.52 8.44 ± 2.33 Na20 2.81 ± 1.31 3.29 ± 1.15 K20 0.59 ± 0.30 0.55 ± 0.30
Pz05 0.34 ± 0.15 0.11 ± 0.02
ppm
Ba 259 ± 139 494 ± 40 Rb 9±6 11 ± 6 Sr 330 ± 227 227 ± 34 y 26±4 15 ± 1 Zr 194 ± 69 80±8 Nb 4±1 7±3 Zn 122 ± 68 101 ± 18 Cu 92±62 70 ±55 I
Ni 113 ± 38 70 ±55 Cr 137 ± 49 38 ± 36
·--
1 =mean mafic volcanic, Wagwater Group (n = 15); 2 =mean mafic volcanic, El Cobre Group (n = 3).
Jamaica high-K andesites occur in the Summerfield
Formation in central Jamaica (Roobol 1976).
A noticeable difference in the Early Tertiary
volcanic activity of the two islands is that the
Wagwater Belt does not contain any volcanic-arc
basalts that match those of Cuba. This difference is
detected in the major- and trace-element chemistry,
where there are significant differences in Ti02,
Al20 3, P20 5, Y, Zr, Ni and Cr (Table 9.2). The
mafic volcanics in the Wagwater Group are higher in
Ti02, P20 5,Y, Zr, Ni and Cr, and lower in AI20 3
than those of El Cobre (Table 9.2) , reflecting a dif
ferent tectonomagmatic setting (Fig 9.4). This is also
highlighted in the MORE-normalized spidergram
where the El Cobre mafic volcanics display a typical
arc basalt pattern, and differ from the Wagwater vol
canics by having lower concentrations ofHFSE (Fig ..
9.6).
There is also a rarity of volcanic rocks of inter-
mediate composition in Jamaica. The rocks in
Jamaica are distinctly bimodal in composition, con
taining tholeiitic intra-plate basalts, and calcalkaline
low- and medium-K dacites (Figs. 9.3, 9.4 and 9.5).
This close temporal and spatial association of intra
plate basalts and convergent-plate dacites led Jackson
and Smith (1979) to conclude that crustal extension
accompanied subduction during the Early Tertiary in
Jamaica, in which the Wagwater Belt was a back-arc
basin. The absence of intra-plate volcanism in eastern
Cuba at that time, and the occurrence of only con
vergent plate volcanics ranging from basalt to dacite,
signifies that the evolution of the arc-back arc system
in Cuba was different to that of Jamaica.
TECTONOMAGMATIC HISTORY
We believe that the shift in K on both islands, from
Late Cretaceous high-K volcanic rocks to Paleogene
3
Q 0
2
0
100
10
0.1
. 01
48 51 54 57 60 63 66 69
Si02
Sr Rb Th Ce Zr Ti02 Sc
72
THE PALEOGENE VOLCANIC ROCKS OF CUBA AND )AMAICA 113
75
Figure 9.5
K20 vs Si02 plot (after LeMaitre 1989) for the
volcanic and altered volcanic rocks of El Cobre
(closed squares) and Wagwater {open squares).
Figure 9.6
MORB-normalized spidergram of basalts from El Cobre (horizontal lines) and Wagwater (vertical lines). MORB data from Sun and McDonough (1989) .
K20 Ba Nb P205 Sm Y Cr
low- and medium-K volcanic rocks, is a result of
changes in plate motion that were taking place as the
Caribbean Plate migrated E and NE. According to
Gill ( 1981), significant shifts in K in arc volcanics
generally signify a change in the melting behaviour
of the mantle in the mantle wedge, brought about
by possible changes in the movement of the sub
ducting plate. In the case of Cuba there is evidence
of a temporary break in subduction at the end of the
Campanian, attributed to the collision of a mature
Cuban arc with the Bahama Platform. Subduction
was not renewed until the Paleocene, but with arc vol
canism being confined only to the Oriente Block. The
direction of subduction during the Cretaceous
remains unresolved (Draper and Barros 1994), but
the arc axis appears to have changed from a NW -SE trend in the Cretaceous to an E-W trend in the
Paleogene (Rosencrantz 1994), suggesting that there
n! ] ..ill! ~ ~ N~ "H'Hl THII!O MILLEJ'I'IUM
,. t= =l
~ 10 r ~-' \1\. ~
=1 "J) .. l! "' ~ ::
E \/ 0 :c =
0.1
.01
100 ~-
10 b-.-.
Rio Grande ·~ --if
l! "' 1t ::: 0 , =
0. 1
r: ~ r
.01
100
r Bransfield
10
"J)
" 3 "" ::;
~ ;:: =
0.1
.01
Sr Rb Th ~b P%05 Hr TiO! Yb
f\.~0 Ba Ta CC" Zr Sm Y Cr
Figure 9. 7 MORB-normalized spidergrams for basalts from Wagwater, Rio Grande and Bransfield. Data for Rio Grande from Gibson et al. (1992) and for Bransfield
from Lawver et al. (1 995). MORB values from Sun and McDonough (1989).
may have been a jumping or flipping of subduction
between the Cretaceous and the Early Tertiary peri
ods. It is the repositioning of the subducting plate and
its motion that could account for the change in K.
In Jamaica, there is no evidence to suggest a cessa
tion of subduction in the Maastrichtian, and neither is
there any indication of a significant shift in arc axis,
nor a major departure in the direction of subduc
tion, which seems to have remained SW to W
(Robinson 1994). Instead, there is evidence that
crustal extension accompanied subduction at the
end of the Cretaceous. This is based on the occur
rence of lamprophyre dikes in the Cretaceous
Paleocene Above Rocks pluton which predate the
volcanics of the Wagwater Group (Jackson et al.
1998). The spatial and temporal relationship of
intra-plate lamprophyres and basalts, and conver
gent plate calcalkaline plutonic and volcanic rocks,
indicates that syn-subduction rifting occurred in
the Early Tertiary, a feature not seen in the Oriente
Block in Cuba. Therefore the change in magma
composition to a more bimodal suite in the Early
Tertiary volcanic rocks of Jamaica may be related
to the crustal extension that accompanied subduc
tion.
The extensional magmatism represented by the
intra-plate basalts in the Wagwater Belt is not report
ed in Cuba, where the basalts show a geochemistry
that is typical of arc-volcanic rocks (Figs. 9.3, 9.4
and 9.6). The Paleogene basalts of]amaica are some
what unusual, in that their chemistry has similarities
to both rift-related basalts (Gibson et al. 1992) and
to enriched back-arc basalts (Stern et al. 1990). The
structural history of the Wagwarer Belt, coupled with
the composition and geographic location of the vol
canic centres (Roobol 1972), prompted Jackson and
Smith (1979) to conclude that the Wagwater Belt
was .aback-arc basin which had resulted from the
splitting of a mature Cretaceous arc. The negative
Nb anomaly seen in the spidergrams would tend to
support a back-arc basin basalt, ·which often shows a
subduction signature during the early opening stages
of the basin (Stern et al. 1990). However, a compari-
400
Wagwaler
100 -
'J!
j . ~ l \ ~ "" 10 -· ~ ;,: .. " ~
j ~·
I -·
=i .::j
.J
400
~ Rio Grande
100
J 'J! .. 3
" it : "" ""
:::1 -1
li ~ 3: ~ ;;
.J
400
Bransfield
100
Ba Th :'ib La Sr PlO~ Zr TiOl Yb.
Rb 1.:20 Ta Ce );d 5m Hf Y
Figure 9.8 Chondrite-normalized spidergrams for basalts
from Wagwater, Rio Grande and Bransfield. Data for Rio Grande from Gibson et al. (1992) and for
Bransfield from Lawver et al. (1995). Chondrite values from Sun and McDonough (1989).
THE PALEOGENE VOLCANIC ROCKS OF CUBA AND ] AMAICA 115
son of MORB- and chrondrite-normalized spider
grams for back-arc basalts and rift-related basalts
shows that the Jamaica basalts compare more
favourably with those of rift-related basalts (Figs 9.7
and 9.8). The patterns compare well with those for
the Rio Grande rift area, showing similar levels of
Light Rare Earth Elements (LREE) and Large Ion
Lithophile Elements (LILE); they are unlike the
enriched back-arc basalts of Bransfield, where the
values are generally lower. -
CONCLUSIONS
The petrology of the Paleogene volcanic rocks of
Cuba and Jamaica indicates that both islands were
experiencing subduction in the Early Tertiary, pro
ducing low- and medium-K volcanics of a tholeiitic
and calcalkaline nature. Cuba comprised a suite of
convergent plate basalts, basaltic andesites, andesites
and dacites, whereas Jamaica contained convergent
plate dacites together with intra-plate basalts. These
intra-plate basalts are the product of crustal thinning
and rifting that took place over a subduction zone in
which lavas of dacitic composition were being
extruded. In contrast, Cuba appears to have under
gone crustal thickening and subduction. The mean
Zr/Y value (Pearce 1983) for the Cuban basalts is
5.6, with ratios ranging from 5.1 to 6.2, suggesting
that Cuba was more likely a continental island arc
rather than an oceanic island arc.
In Jamaica, the crustal thickness at the end of
the Cretaceous is estimated to be greater than 30 km Qackson et al. 1989), using the Rb-Sr thickness grid
of Condie (1973). This would indicate that the crust
underlying Jamaica was more continental than
oceanic in nature, which could account for some of
the continental basalt chemical signatures seen in the
Paleogene basalts that make them comparable with
those of the Rio Grande rift. The negative Nb anom
aly in the MORB-normalized spidergram indicates
that a subduction component contributed to the
composition of the intra-plate basaltic magma. We
believe that the Paleocene-early Eocene rifting and
11\B• ~·~ hi.1IJIIII lli>ETii-ICl Mlti£:-.,..IUM
_.,_ iw- rifi:-rdared basalt volcanism that occurred
ill }:unaica signalled the break-up of Jamaica from
Cenrral America. This rifting may have been a pre
cursor to the initial opening of the Cayman Trough,
as a paleogeographic reconstruction of Jamaica in
relation to the Cayman Trough in the Eocene places
Jamaica next to the mid-Cayman spreading centre
(Rosencrantz and Sclater 1986) .
ACKNOWLEDGEMENTS. This paper stemmed from a visit
made by Trevor jackson to Cuba in November 1996 as a
member of a field excursion to the Oriente Block by the IGCP
Project 364 working group. The authors thank Trevor McCain
(UWI) for thin section preparation; the staff of the Cam borne
School of Mines (CSM), especially Fiona Thomas (XRF); and
the Inter American Development Bank (!DB) for funding
Trevor jackson's visit to CSM in August 1997, during which
much of the analytical work was undertaken. The authors
thank Gautum Sen (FlU) for his con-structive comments on the
manuscript.
REFERENCES
Ahmad, R, N. Lal, and P.K. Sharma. 1988. Fission
track age of ignimbrite from Summerfield
Formation, Jamaica. Caribbean jour(lal of
Science 23:444-48. Condie, K.C. 1973. Archean magamatism and crustal
thickening. Bulletin of the Geological Society of
America 84:2981-92. Diaz de Villavilla, L., I. Milia, and E. Domiguez. 1998.
Geochemical pecularities of the volcanic
sequence of Central Cuba: comparison with the Caribbean region. 15th Caribbean
Geological Conference, Kingston, jamaica (late
abstract).
Donovan, S.K., and T.A. Jackson. 1994. Caribbean
Geology: An Introduction. Kingston, Jamaica:
University of the West Indies Publishers'
Association.
Donnelly, T.W, Beets, D., Carr, M.J., et al. 1990.
History and tectonic setting of Caribbean
magmatism. In The Caribbean Region, ed. G.
Dengo, and J.E. Case, 339-74. Volume H of
The Geology of North America. Boulder,
Colorado: Geological Society of America.
Draper, G. and Barros, J.A. 1994. Cuba. In Caribbean
Geology: An Introduction, ed. S.K. Donovan
and T.A. Jackson, 65-86. Kingston, Jamaica:
University of the West Indies Publishers'
Association.
Gibson, S.A. et al. 1992. Asthenosphere-derived mag
matism in the Rio Grande rift, western USA:
implications for continental break-up. In
Magmatism and the Causes of Continental
Break-up, ed. B.C. Storey, T. Alabaster, and
R.J. Pankhurst, 61-90. Geological Society
Special Publication 68, The Geological Society.
Gill, J.B. 1981. Orogenic Andesites and Plate Tectonics.
New York: Springer-Verlag.
Green, G.W 1977. Structure and stratigraphy of the
Wagwater Belt, Kingston, Jamaica. Overseas
Geology and Mineral Resources 48:1-21
Irvine, T.N., and WRA. Barager, 1971. A guide to the
classification of the common volcanic rocks.
Canadian journal of Earth Sciences 8:523-48.
Isaacs, M.C. and T.A. Jackson. 1987. The mineralogy
and geochemistry of the plutonic rocks from
Jamaica. In Proceedings of a Workshop on the
Status of jamaican Geology, ed. R. Ahmad,
95-106. Geological Society of jamaica Special
Issue.
Iturralde-Vinent, M.A. 1994. Cuban geology: a new
plate tectonic synthesis. journal of Petroleum
Geology 17:39-70.
I~rralde-Vinent, M.A. 1996. Cuba: el archipielago , volcanico Paleoceno-Eoceno Medio. In
Ofiolitas y Arcos Volcdnicos de Cuba, ed. M.A.
Iturralde-Vinent, 231-46. UNESCO-I GCP
Project 364 Caribbean Ophiolites and
Volcanic arcs, Special Contribution 1.
Jackson, T.A., 1977. The petrochemistry of the vol
canic rocks of the Wagwater Belt, Jamaicay
Wl. PhD diss., University of the West In~ies.
Jackson, T.A., and T.E. Smith. 1978. Metasomatism in
the Tertiary volcanics of the Wagwater Belt,
Jamaica. Geologie Mijnbouw 57:213-20.
Jackson, T.A., and T.E. Smith. 1979. The tectonic sig
nificance of basalts and dacites in the
Wagwater Belt, Jamaica. Geological Magazine 116:365-74.
Jackson, T.A., T.E. Smith, and M.C. Isaacs. 1989. The
significance of geochemical variations in the
Cretaceous volcanic and plutonic rocks of
intermediate and felsic composition from
] amaica. journal of the Geological Society of jamaica 26:33-42.
Jackson, T.A., ].F. Lewis, P.W Scott, and P.A.S.
Manning. 1998. The petrology oflampro
phyre dikes in the Above Rocks granitoid,
Jamaica: evidence of rifting above a subduc
tion zone during the early Tertiary. Caribbean
journal of Science 34:1-11.
Kysar, G., D. Green, M. Perez, I. Mendez, and R.
Rodriguez. 1998. Igneous rocks of the Sierra
Maestra, southeastern Cuba; new major and
trace element analyses. Abstract, 15th
Caribbean Geological Conference, Kingston,
Jamaica, June 29-July 2, 1998, Contributions to Geology, University of the West Indies,
Mona, 3, 84.
Lawver, L.A., R.A. Keller, M.R. Fisk, and J.A. Strelin.
1995. Bransfield Strait, Antarctic Peninsula:
active extension behind a dead arc. In Backarc Basins: Tectonics and Magmatism, ed. B. Taylor,
315-42. New York: Plenum Press.
LeMaitre, R.W, ed. 1989. A Classification ofigneous Rocks and a Glossary ofTerms. London:
Blackwell Scientific Publications.
Pearce, J.A. 1983. Role of the sub-continental litho
sphere in magma genesis at active continental
margins. In Continental Basalts and Mantle
Xenoliths, ed. C.J. Hawkesworth, and M.J.
Norry, 230-49. Shiva, Nantwich.
Pearce, ] .A., and] .R. Cann. 1972. Tectonic setting of
THE PALEOGENE VOLCANIC ROCKS OF CUBA AND jA.'.t~ iU '. -i
basic volcanic rocks determined using trace
element analyses. Earth and Planetary Science
Letters 19:290-300. .
Pindel, J.L. 1994. Evolution of the Gulf of Mexico and
the Caribbean. In Caribbean Geology: An
Introduction ed. S.K. Donovan and T.A.
Jackson, 13-39. Kingston, Jamaica: University
of the West Indies Publishers' Association.
Robinson, E. 1994. Jamaica. In Caribbean Geology: An Introduction, ed. S.K. Donovan and T.A.
Jackson, 111-27. Kingston, Jamaica:
University of the West Indies Publishers'
Association.
Roobol, M.J. 1972. The volcanic geology of]amaica.
In Transactions of the ffh Caribbean Geological
Conference, Margarita, Venezuela, 1971, ed. C.
Petzall, 100-107.
Roobol, M.]. 1976. Post-eruptive mechanical sorting
of pyroclastic material: an example from
Jamaica. Geological Magazine, 113:429-40.
Rosencrantz, E. 1994. Basement structure and tecton
ics in the Yucatan Basin. In Ofiolitas y Arcos Volcdnicos de Cuba, ed. M.A. Iturralde-Vinent,
36-47. UNESCO-IGCP Project 364
Caribbean Ophiolites and Volcanic arcs,
Special Contribution 1.
Rosencrantz, E. and Sdater, ] .G. 1986. Depth and age
of the Cayman Trough. Earth and Planetary Science Letters 79:133-44.
Stern, R.J., et al . 1990. Enriched back-arc basin basalts
from the northern Mariana Trough: implications for magmatic evolution of back-arc
basins. Earth and Planetary Science Letters 100:210-25.
Sun, S-s, and WF. McDonough. 1989. Chemical and
isotopic systematics of oceanic basalts: impli
cations for mantle composition and processes.
In Magmatism in the Ocean Basins, ed. A.D.
Saunders, and M.J. Norry, 313-45. Geological Society Special Publication 42. The Geological
Society of London.
Winchester, ].A., and P.A. Floyd. 1977. Geochemical
discrimination of different magma series and
their differentiation products using immobile
elements. Chemical Geology 20:325-43