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.

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