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thesis entitled

The Origin of Silicic Domes in the Vicinity of the Makiling
Stratovolcano in the Macolod Corridor, Philippines: Evidence
From Bulk Chemistry, Mineralogy and Oxygen Isotopes

presented by

Melissa Sue Wilmot

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THE ORIGIN OF SILICIC DOMES IN THE VICINITY OF THE MAKILING
STRATOVOLCANO IN THE MACOLOD CORRIDOR, LUZON, PHILIPPINES:
EVIDENCE FROM BULK CHEMISTRY, MINERALOGY AND OXYGEN
ISOTOPES
By

Melissa Sue Wilmot

A THESIS
Submitted to
Michigan State University
in partial fulfillment of the requirements
for the degree of
MASTER OF SCIENCE
Department of Geological Sciences

2005

ABSTRACT
THE ORIGIN OF SILICIC DOMES IN THE VICINITY OF THE MAKILING
STRATOVOLCANO IN THE MACOLOD CORRIDOR, LUZON, PHILIPPINES:
EVIDENCE FROM BULK CHEMISTRY, MINERALOGY AND OXYGEN
ISOTOPES
By
Melissa Sue Wilmot
The origin of high-silica magmas in areas lacking continental crust is not well-
understood. The Macolod Com’dor on Luzon Island of the Philippines provides an ideal
area to study to this problem. Two end-member models, partial melting of previously
emplaced magma batches and fractional crystallization, have been developed to explain
the formation of high-silica magmas. The Silicic domes (Bulalo, Bijang, Olila and
Calamba) examined in this study are located near the Makiling Stratovolcano. The
mineralogy and chemical composition of Bulalo, Bijang and Olila are very similar, while
Calamba shows some slight differences. Most of the evidence developed in this study
supports partial melting of discrete batches of previously emplaced crystallized magma as
the likely source for the high-silica magmas composing the domes. The composition of
domes can only be produced through the partial melting of an andesitic/dacitic source.
The Sr concentration in the domes is too high to indicate the fractionation of large
amounts of plagioclase. Neither the An content of plagioclase phenocrysts nor the Sr/Ba
ratio indicates that fractional crystallization could have produced the chemistry of the
domes. The observed difference in REE patterns of Calamba may be due to a larger
degree of partial melting. The oxygen isotope values are similar for the three domes
analyzed, indicating a similar source for the dome magmas. The high-silica Mt. Makiling

samples most likely originated from a different source magma than the dome samples.

ACKNOWLEDGMENTS

One of the most important lessons that I learned during the process of completing
my thesis is that, despite the single name on the cover, a thesis is actually the combined
effort of many people, both directly and indirectly. I am grateful to all of those people,
though only a few are listed here. First, I need to thank my committee, Tom, Lina,
Duncan and Tim. The input and support that they gave me all along the way was
invaluable. I would also like to acknowledge Jake Eaton and Dr. John Valley, from the
University of Wisconsin-Madison- Jake for all of his help with oxygen isotopes, and Dr.
Valley for allowing his student to help me out so much! The petrology group at
Michigan State University was great because they were always ready to lend moral
support when needed, as well as their expertise in the field of being a graduate student
trying to complete a thesis! Thanks especially to Karen, Dave, Ela, Beth and Chad.

Finally, to my parents, without their love and support, I would not be where I am today.

iii

TABLE OF CONTENTS

INTRODUCTION... . .

DATA COLLECTIONANDANALYSIS...

DataCollection............................... ..
Petrographic Analysis... ..

TraceElements....

Mineral Chemisuy....................fIIIIII.’IIIIIIII.’IfZIIIL'IZIIIILILII'.77.2.14

Plagioclase...........

Amphiboles...... .............fil.I.'II.'I'..°.I."...".'..".'..'..."..fff'fj'f.'I..".'..".'.I'.'.17
.17
..18

....19

Pyroxenes.........

Matrix Glue--..................IZIIIIZIIIIIIIIIIIIIII'IIIIIIZIICIIIIIIIIIIII'
Oxygen Isotope Data

DISCUSSION...

Comparison of the Domes arid Makiling
Fractional Crystallization vs. Partial Melting
Magma Mixing...

Eruption of the Magma/Formation of the Domes

APPENDIX 1- Petrographic Descriptions
Bijang...
Bmflo .mnnumnnu
Olila... ..

Calamba......
APPENDIX 2- Figures
APPENDIX 3- Tables............

iv

”:10
Bulk Chemical Composition... ....12
MajorElements............................................ 12

.13

14

.........20
......20
......21
......24

...25

...29
.......3O
....31

.33
...35
...38
...67

...96

LIST OF TABLES

Table l-Ages ofSelectedDomes fromtheMacolodCorridor............ . ..
TableZ-ThermobarometryResults-Calamba..............................................
Table3-OxygenData............................................
Table4a-BulkChemicalAnalyses-MajorElements...................

Table4b-BulkChemicalAnalyses-TraceElements......................................
Table 5-PlagioclaseMajorElementAnalyses..............................................
Table6-HornblendeAnalyses...............................................................
Table7-PyroxeneAnalyses...................................................................
Table 8- Fe-TiOxide Analyses...................
Table9a-TraceElements-Plagioclase.........................

Table 9b- Trace Elements- Enclave Plagioclase..............................

...68

...69

...71

...72

...74

...80

...87

...89

...93

...95

.95

LIST OF FIGURES

Figure 1- Map of the Philippines showing the location of the plates and the features
associated with them. Note: the author refers to the Eurasian Plate as the Sunda
Plate in this diagram (Bacolcol, 2003)... ..39

Figure 2- Location of the Macolod Corridor: It is located between the Bataan and
Mindoro segments of the Luzon Are. On this diagram, the Eurasian Plate has
been labeled as the South China Sea Plate. The Mindoro-Palawan terrane in the
southwest part of the islands contains a large block composed of continental
crust However, it is located well south and west of the Macolod Corridor, in
which the presence of continental crust has not been observed (Defant et al.,

Figure 3- Location of the Macolod Corridor in relation to Taal Volcano and the Laguna
deBay caldera (Sudo et al., 2001)... 4.1

Figure 4- Close-up view of the Makiling volcano area and the domes associated with it
(Oles, 1991)...... ....42

Figure 5- Examples of plagioclase grains from the four domes: a. Well-zoned grain from
Calamba (020517-2d); b. Grain from Olila (020522-56tav) that is highly
embayed, possibly indicative of disequilbn'um; c. Grain from Calamba
(020517-2d) that has a sieve-like texture in the center surrounded by a rim; d.
Grain from Olila (020522-2d) with a well-defined outer rim... .43

Figure 6- Example of two glomerophyric clots: a. Clot containing only plagioclase
grains, from Olila (020522-53); b. Clot from Calamba (020517-2d) that
contains several different mineral types grown together... ...44

Figure 7- Examples of minerals found in the four domes- aCommon hornblende grain
from Bijang (0205 18- 1c); b. Large opaque grains from Olila (020522-53); c.
Orthopyroxene grain from Bulalo (020522-51)H d. Clmopyroxene grain from
Calamba(020517-2m)... . . . .. ......44

Figure 8- Examples of phenocryst differences from the two different sizes of enclaves: a.
Small enclave from Bulalo (020522-51); b. Large enclave from Olila (020522-
51tav)- Note the difference in the grain sizes, with the smaller enclave
composed of larger needle-like plagioclase grains, most with well-defined
compositional rims, while the larger enclave has smaller needle-like plagioclase
grains with larger phenocrysts of hornblende and plagioclase. .. ...45

Figure 9- Bulk chemical compositions of the domes and enclaves- classifications based
on Le Bas et a1. (1986). Filled symbols: Enclaves; Open symbols: Domes. . . 46

Figure 10- Major element diagrams of the host and enclave compositions. The host
composition of Calamba is different than the other three domes. The enclave
compositions ofeach dome are very similar... .47

Figure 11- Trace element diagrams of the host and enclave compositions. The host
compositions of Calamba display some differences compared to the other
threedomes... .. 48

Figure 12a- REE diagrams of dome and enclave compositions, based on Sun and
McDonough (1989), normalized to chondrite compositions. The host
compositions of all four domes display a concave upward trend indicative of
a depletion in the MREES. The enclaves do not show this depletion, except
those from Calamba... ...49

Figure 12b- Diagram showing the difference in the MREEs and LREES between Calamba
and the other three domes. The difference in MREES may be attributed to
the presence of amphibole in the source. The MREEs have higher partition
coefficients into amphibole than the other REES, and are represented by Dy
on the diagram. The difference in LREEs may be attributed to different
degrees of partial melting. Values were normalized to their mantle source
values, per the IgPet program... ..50

Figure 13- Trace element diagram normalized to primitive mantle, based on Sun and
McDonough (1989). These diagrams show that the four domes lack a Eu
anomaly... 51

Figure 14- Diagram showing An content of plagioclase grains from the four domes.
Generally, the trend is a decrease in An content from the center of the grain to
the edge. One grain from Bijang and one grain from Olila shows what
appears to be reverse zoning, but could also be the result of analyzing two
different grains that have grown together. Also of note are the two grains
from Calamba with cores of An > 55%. The tie lines connect the center of
grains with the edge ofthe same grain... ..52

Figure 15- Diagram of An compositions of plagioclase grains from the enclaves of
Bulalo, Olila, and Calamba. Bulalo and Olila contained two different sized
enclaves, although it is likely that the area interpreted as a small enclave in
Olila was not one,based on the low An content ofthe grains... .....53

Figure 16a- Diagrams showing the Sr and Ba concentrations and Sr/Ba ratios in
plagioclase grains from Calamba, Olila and Bulalo. The bottom diagrams
contain data from three grains (two from Calamba, one from Bulalo) that
contained centers with much higher An content than the edges. Despite the
similar Sr/Ba ratio of the centers of the three grains in the bottom diagrams,
the An content of the center of each one is very different: 83%, 64% and
55% ............................................................................................................ 54

vii

Figure 16b- Diagram of Sr and Ba compositions as well as Sr/Ba ratios of enclave grains
from Olila and Bulalo. All three grains were located in small enclaves... ..55

Figure 17a- Amphibole major element chemistry- there is no noticeable difference
between the chemical composition of the amphiboles of the domes, or
betweenthehostandenclave... 56

Figure 17b- Magnesium number of amphibole vs. SiOz content- there is no correlation
between the magnesium number and silica content, or between the enclaves
and the host... ...57

Figure 18a- Pyroxene composition- there is no distinction between the orthopyroxenes of
the four domes. The clinopyroxenes of Calamba are chemically similar as
well- except for one outlier, 020517-2h- pyx #9... ...58

Figure 18b- Plotting enstatite percentage vs. Mg # shows that there is not a wide variation
of either in the orthopyroxenes of the four domes, or of the clinopyroxenes of

Figure 19- Glass analysis vs. bulk chemical composition. The host glass does not show
signs of mingling- the silica values are higher than the bulk composition. The
enclave glass fiom the small enclaves of Olila and Bulalo show some
evidence ofmingling due to the high silica values... ...59

Figure 20- Oxygen isotope values for three domes- 5180 values for the minerals are very
similar, indicating that the values have not been reset. The whole rock values
are also very similar, indicating that the three domes originated from a similar
source... ....60

Figure 21a- Plots comparing the chemical composition of the domes with those from
Makiling. The dome compositions and the mafic enclaves are represented by
the gray areas. It can be seen from this diagram that the dome samples have a
major element chemistry that is similar to the Makiling samples... ..61

Figure 21b- Diagrams comparing the REE concentrations of the domes and Makiling The
mafic samples are very similar to the mafic enclave compositions of the
domes. The Silicic samples from Makiling do not show the same depletion in
MREES as those from the domes... ...62

viii

Figure 22- Experimental fractional crystallization trends- solid line represents work of
Grove et a1 (2003) and Muntener et a]. (2001) with a basaltic starting
composition at varying water pressures and saturation; dotted line represents
the trend with an andesitic starting composition (Grove et al., 2003); dashed
line represents fractionation trend with andesitic starting composition at
shallow pressures (Grove et al., 2003); dotted/dashed line represents
fractionation at 1 GPa of a tholeiitic basalt (Villeger, et al., 2004). While the
work of Villeger comes close to reproducing the composition of the domes
and Makiling, it is through extremely high amounts of fractionation, >90%..63

Figure 23- Diagram representing the experimental products of partially melted source
rocks of varying composition (Patino-Douce, et al., 1999). The domes do not
fall within any fields, but come closest to being reproduced by partial melting
of a meta-andesite/dacite... . .. .. . . . ..64

Figure 24- Diagram of Sr/Ba vs %An- There is a general trend of increasing Sr/Ba with
increasing %An, up to 50% An. This is indicative of chemistry changes in the
plagioclase reflecting changes in melt composition rather than changes in
pressure or water content (Browne et al., 2004). The second trend observed is
a ratio of 6 for a variety of An compositions. The points found in this second
group come from two grains from Calamba and one grain from Bulalo that
contain centers with high An. These points most likely represent centers of
grains that originated in a more mafic magma. In this case, the change in the
major element composition of the plagioclase grains maybe attributed to
processes other than compositional changes of the magmas, such as a change
in water pressure or temperature (Ginibre et al., 2002)... ...65

Figure 25- Partial melting and eruption model- a. Dehydration melting of the mantle
wedge leads to the formation of a mafic magma. This mafic magma travels
through the wedge and encounters a solidified or partially solidified body of
calc-alkaline andesite. The heat from the mafic magma partially melts and
mobilizes the more siliceous product. This siliceous magma may travel
through the crust and erupt at the surface, or it may stall out, requiring an
additional influx (b) of hot, mafic magma to cause the eruption. (Not to scale)

Images in this thesis are presented in color.

ix

INTRODUCTION

Silicic volcanic rocks are abundant in continental arcs, but not widely recognized
in oceanic arcs. It has only recently been recognized that Silicic rocks can be found in
abundance in areas lacking continental crust. Areas such as the Kermadec Arc (Smith et
al., 2003a, Smith et al., 2003b) and the Izu-Bonin Arc (Tamura and Tatsumi, 2002) are
currently being studied. The Silicic domes in the vicinity of the Makiling Stratovolcano
in the Macolod Corridor on Luzon Island of the Philippines, are another example and
provide an ideal setting to investigate how Silicic magmas form in oceanic arcs. The
composition and origin of these domes are the focus of this study.

The study of the formation of high-silica magmas is important for many reasons.
Understanding the evolution of high-silica magmas in oceanic arcs may provide insight
into how continental crust evolved. Also, high-silica magmas often erupt with highly
explosive force due to the high viscosity and gas-content of these magmas. Because
many people live in close proximity to areas actively erupting high-silica magmas, an
understanding of how they form may provide insight into how to predict the eruptions.

There are two end-member models that have been used to explain the evolution of
high-silica magmas in areas lacking continental crust: fractional crystallization of mantle
derived magmas, and partial melting of previously emplaced magma (Riley et al., 2001;
Tamura and Tatsumi, 2002; Singer et al., 1992; Brophy and Dreher, 2000). In one model
of fractional crystallization, a magma evolves through the crystallization of early formed
minerals, either by side-wall crystallization or crystal settling. This allows for a more
siliceous melt to form. This process is considered to be unrealistic by some workers due

to the large amount of fractionation needed. A variation of the crystal fractionation

model involves the formation of a partially-solidified layer that advances downward
through the chamber (Brophy and Dreher, 2000). In this model, the fractionated liquid is
trapped in this layer until it has crystallized enough to become rigid. At this point, the
layer may fracture, allowing the more evolved liquid trapped between the crystals to
become segregated from the other components. This becomes the more evolved liquid
that eventually may erupt at the surface or stall in the crust (Brophy and Dreher, 2000).

Partial melting is the other end-member model. In arc regions, recent workers
have suggested that an influx of magma may cause partial melting of plutons of varying
compositions (e. g. Tamura and Tatsumi, 2002; Tamura et al., 2003; Riley et al., 2001).
Early work focused on the formation of high-silica magma through the partial melting of
basaltic and andesitic rocks. Beard and Lofgren (1991) performed several melting
experiments in which they began with rocks of those compositions and melted them in
anhydrous and hydrous conditions at different pressures. They were able to produce melts
of granodioritic and trondhjernitic composition. Based on the Beard and Lofgren (1991)
experiments, Tamura and Tatsumi (2002) suggested that hydrous calc-alkaline andesites
emplaced in the crust were the source of the rhyolites of the Izu-Bonin arc. In Tamura
and Tatsumi’s (2002) model, the magmas crystallize and stall before they reach the
surface because high water content decreased the liquidus temperature. An influx of hot,
basaltic magma reheats and partially melts these calc-alkaline andesites, remobilizing
them and erupting rhyolitic lava on the surface.

The purpose of this paper is to determine the processes that led to the formation of
four of the domes located near the Makiling stratovolcano. The main question to be

addressed is: How did the high-silica magma form? A second question is: How are the

four domes related to one another and to the Makiling stratovolcano? Data used in this
study include: petrographic analysis, bulk chemsitry, mineral phase and glass

composition, and oxygen isotope values of the whole rock and individual minerals.

GEOLOGIC SETTING

The Philippine Archipelago is located in an oceanic are that also contains
ophiolite and continental terranes (figure 1), although these compose only a small part of
the islands as part of the Palawan Tenane(f1gure 2) (Knittel et al., 1988). The Philippine
archipelago lies south of Taiwan, between the South China Sea to the west and the
Philippine Sea to the east. This area is geologically complex because it is situated
between two opposing subduction zones involving the Eurasian Plate and the Philippine
Sea Plate, in an area of intense deformation (Cardwell et al., 1980). The Philippine
Trench and East Luzon Trough occur off the east coast of Luzon, the northernmost and
largest island in the Philippines. These formed due to the westward subduction of the
Philippine Sea Plate. The Manila, Negros and Cotabato Trenches occur off the west
coast, and formed due to the eastward subduction of the Eurasian Plate (Bautista et al.,
2001). A series of N-S trending faults formed as a result of the compressional and
shearing forces caused by the opposing subduction zones. The longest area of faulting is
the Philippine Fault Zone, which extends from Mindanao in the southern Philippines to
northern Luzon (Bautista et al., 2001).

The subduction zone located off the east coast of Luzon has been the cause of
Late Miocene to Recent volcanic eruptions (Mukasa et al., 1987). The subduction at the
East Luzon Trough is not currently related to active volcanism, most likely due to the
shallow angle of subduction (Defant et al., 1989). In contrast, the western coast of Luzon
is the site of active subduction-related volcanism, which formed the “Luzon are” that

extends from Taiwan to Mindoro. The Luzon arc is divided into five segments based on a

difference in tectonic settings and magma evolution processes: Mindoro, Bataan, N.
Luzon, Babayan and Taiwan (Defant et al., 1989).

The Silicic domes examined in this study occur near the Makiling Volcano in the
Macolod Conidor, which is an extensional zone between the Mindoro and Bataan
segments of the Luzon Arc (figure 2) (Sudo et al., 2001). The Macolod Corridor
stretches 60 km across Central Luzon, an area which contains no continental terranes
(Defant et al., 1989). The Macolod Corridor consists of a basement composed of
intrusive bodies and limestone. The oldest rocks in this area include a sequence of
Paleocene-Oligocene San Juan metavolcanics and metasediments, and early to mid-
Miocene San Juan quartz diorite (Sudo et al., 2001; Oles, 1991). The initiation of the
most recent episodes of volcanism in the Macolod Corridor is not well-constrained, with
estimates ranging from 1.8 to 0.6 Ma. Volcanism continues through the present (Defant et
al., 1989; Sudo et al., 2001). The formation of the Corridor is still a matter of debate,
although the general consensus is that it is a pull-apart rift zone (Bautista et al., 2001;
Mukasa et al., 1994; Sudo et al., 2001). This may have led to the extensive faulting that
is observed in the Corridor. Bulalo Dome alone is surrounded by several normal faults
(Aquino, 2004).

Many types of volcanic activity have occurred in the Corridor. Other volcanic
deposits in this area include basaltic scoria cones and maars, active solfatara fields
(fumarole-type structures characterized by sulfurous emissions (Bates and Jackson,
1957)) ash-flow tuffs, and stratovolcanoes (Forster et al., 1990, Sudo et al., 2001). Two
large calderas occur in the Corridor: Laguna de Bay and Taal Volcano (Figure 3). The

youngest Silicic samples from Laguna de Bay have been dated at 42-47 ka and 27-29 ka

(Catane and Arpa, 1998). Mount Taal has been active as recently as 1969, although this
eruption was mostly basaltic in character (Sudo et al., 2001). The three stratovolcanoes
that occur in the Corridor are Mt. Banahaw, Mt. Makiling, and Mt. Malipunyo. A series
of monogenetic volcanoes that erupt basaltic magma are also located here. These
monogenetic volcanoes include 42 scoria cones and 36 mars that have been dated at
1.05 :1: 0.05 Ma and 0.84 :L- 0.13 Ma (Sudo et al., 2001).

Several domes are found in the area between Laguna de Bay and Taal Lake
(figure 4). The domes to be investigated in this study are all located near Mt. Makiling, a
large stratovolcano composed of andesitic and dacitic lava flows, airfall deposits and
pyroclastic flows (Sudo et al., 2001). No data on the age of the volcanic deposits of
Makiling are available. The domes in this area include Mt. Bijang, Calamba (Mt.
Mapinggoy), Olila, Bulalo, and Trapiche (Tanuaun Hill) (figure 4), none of which have
been previously studied. Ar/Ar dating performed on Trapiche, Bulalo and Bijang yielded
ages of 43il7 ka, 15:1:7 ka and 66i14 ka respectively (table 1) (Heizler, personal

communication, 2003).

DATA COLLECTION AND ANALYSIS

Data Collection

Of the many obsidian domes present throughout the Macolod Corridor (Sudo et
al., 2001), many of them are not accessible. The six domes that were sampled had been
exposed in areas such as road cuts and quarries, making sample collection possible. Four
of these domes (Bulalo, Olila, Bijang and Calamba) were chosen as the focus of this
study because they had been recently exposed by construction projects, providing easy
access to fresh samples. Also, the domes chosen cover a wide area and contain abundant
mafic enclaves.

Data were collecwd from samples from each of the four domes by several
methods. Bulk chemical analysis of both major and trace elements was carried out using
X-Ray Fluorescence (XRF) and Laser Ablation Inductively Coupled Plasma Mass
Spectrometry (LA-ICP-MS) at Michigan State University. Individual mineral
phenocrysts and matrix glass were analyzed for major and trace elemental compositions
using the Electron Microprobe Analyzer (EMPA) at the University of Michigan. LA-ICP-
MS was used as well. Oxygen isotope data for minerals from Calamba, Bulalo and
Bijang were collected using the C02 laser fluorination/mass spectrometer at the
University of Wisconsin-Madison.

Bulk chemical analysis was performed on glass disks composed of fused samples.
The disks were prepared following the procedure outlined in Hannah et al. (2002) and
Viray (2003). Where possible, the host rocks were separated from the enclaves during
the sample preparation process. Enclaves that were large enough were analyzed

separately from the host samples.

Minerals and glass from the matrix were analyzed for major elements and some
trace elements using EMPA. Mineral phases analyzed included plagioclase, hornblende,
pyroxene, magnetite and ilmenite. For these phases, analyses were done one point at a
time using a Cameca SX 100 EMPA. It was equipped with five wavelength
spectrometers using an accelerating potential of 15 kV. Other settings, including beam
spot size, counting time, and beam strength varied based on the phase being analyzed.
Glass from the host matrix and the enclaves was also analyzed using EMPA. Analyses of
glass in the matrix were carried out using two different methods. If there were an area in
which a section of glass was free of microlites, one or two points were taken in that area.
This was commonly used in the enclaves because there were clear areas of glass between
the needle-like plagioclase grains and phenocrysts. In the host samples, a S-um beam
was used, and points were analyzed at 15-pm increments. Areas of 3 points by 4 points,
or 45 pm by 60pm were analyzed in this way. A lower beam strength was used to
analyze the glass as well. Both of these analytical methods limited the migration of
volatile elements such as Na, and improved the results of the analyses. The compositions
of each point were then examined, bad totals eliminated, and the rest averaged to obtain
the glass compositions.

Trace elements were collected from plagioclase and hornblende using LA-ICP-
MS. Data were collected from selected plagioclase grains that had been analyzed using
the microprobe. The same points were analyzed using a glass standard (NIST 612) and
the Ca concentrations collected from EMPA as an internal standard. The laser was
focused to a 25 um sampling size and penetrated the sample at a rate of 3 urn/sec. The

peak intensities of 88Sr, l3'i‘Ba and 44Ca were collected.

Oxygen isotOpe values were obtained using C02 laser fluorination/mass
spectrometry. The procedure followed in order to prepare the dome samples for oxygen
isotope analysis was carried out with an emphasis on collecting zircons. Zircons are the
preferred mineral for analysis because they record the initial values for a magma and are
resistant to reset by subsequent processes. Sample preparation began with the crushing of
large amounts of sample. Approximately 25 pounds of sample from each of three domes
was crushed and ground in the same method as for the bulk chemical analysis. Such
large amounts were needed in order to collect enough zircons for analysis, and a
sufficient amount of sample was only available for Calamba, Bijang and Bulalo. The
second step was mineral separation, with an emphasis on separating out zircons. The
crushed sample was separated by the following method: First, the sample was shaken
down a gold table to separate the light from the heavy minerals. Once the mineral
separates were dry, a hand magnet was used to separate out the magnetic minerals in
preparation for the next step, separation using a Franz Isodynamic Magnetic Separator.
The samples were separated further using methylene iodide. Methylene iodide contains
a known density in which zircons were expected to sink while the less dense minerals
would float, allowing for the separation of zircons from the rest of the minerals. Finally,
the grains were separated out by hand using a microscope and tweezers. Because zircons
were not found in a large enough abundance to analyze, hornblende, feldspar and

magnetite were separated out for oxygen isotope analysis.

Petrographic Analysis

The mineral assemblages of each dome are very similar, with Bijang, Bulalo and
Olila containing an almost identical mineral assemblage, and the Calamba samples
containing a slightly different assemblage (for a complete description of the mineralogy
of each dome, see Appendix 1). The samples from Olila, Bulalo and Bijang are
porphyritic. Phenocrysts compose 15-25% of the samples. The matrix is glassy and
microlitic. Mafic enclaves of varying sizes are found in Olila and Bulalo. None were
observed in the Bijang samples. Plagioclase composes up to 70% of the phenocrysts in
each of the domes (figure 5). Generally, the grains are euhedral, with sizes that range
from 0.2 to 2.5 mm, and are equally distributed. Plagioclase grains with a sieve texture
and/or deep embayments (figure 5b) are rare in all three domes, as are grains with a
sieve-textured core and well-zoned rim (figure 5c). Most of the plagioclase grains also
contain slight embayments and rounded edges, possibly indicative of slight
disequilibrium. A few of the grains contain well-defined outer rims, although these are
more common in the enclaves (figure 5d). A glomerophyric texture is common in all
three domes, with many of the larger plagioclase grains found in clusters (figure 6a).
Occasionally these clusters also contain other minerals, including hornblende, opaques,
and, rarely, pyroxene. These clusters may represent pieces of wall-rock that were taken
up during the eruption and are not part of the host magma.

The other minerals found in Bulalo, Olila and Bijang include hornblende, Opaques
and orthopyroxene, in order of abundance. Homblende (figure 7a) composes 25-30% of
the phenocrysts. The hornblende grains are mostly euhedral, with sizes that range from

0.2 to 0.7 mm. The grains also contain slight embayments and rounded edges, with rare

10

sieve textures. The opaque grains (figure 7b) observed in the domes are magnetite. No
ilmenite was analyzed in these three domes. Magnetite composes ~5% of the phenocryst
assemblage of the domes. These grains are generally subhedral to anhedral. The larger
opaque grains are around 0.7 mm, although most of the grains are much smaller. The
opaques rarely contain embayments. Orthopyroxene (figure 7c) is the least abundant
mineral in the three domes, composing less than 5% of the assemblage. Only Bulalo
contains more orthopyroxene than opaques, although the difference is very small. The
pyroxenes are generally euhedral, with sizes as large as 0.7 mm. However, most are
significantly smaller, with an average size of 0.1 mm. The larger grains typically show
signs of resorption, while the smaller grains typically do not.

The Calamba samples are petrographically different than the other three domes.
The matrix of most of the Calamba samples is devitrified, contrary to the other domes.
Only one sample (020517-2d) contains a glassy matrix. The major petrographic
difference between Calamba and the other three domes is that amphibole is only a minor
mineral phase, composing <1% of the assemblage. Instead, pyroxene is the second most
abundant mineral phase, composing 25% of the phenocryst assemblage. Also different
than the other three domes is the presence of both clinopyroxene (figure 7d) and
orthopyroxene. Exact proportions can not be estimated due to the difficulty distinguishing
the two types visually, however. The pyroxenes are generally larger than those found in
the other three domes, with sizes ranging from 0.05 to 0.23 mm. The third most abundant
phase is the opaques, and both magnetite and ilmentite are present in the Calamba
samples, in contrast to the other three domes. The textures of the minerals from

Calamba generally are similar to the other domes.

ll

Mafic enclaves are present in Olila, Calamba and Bulalo (figure 8). The enclaves
observed in Olila and Bulalo vary in size. The major differences between the large and
small enclaves are the size of the grains and the textural evidence of interaction with the
host magma (see appendix 1 for an in-depth description of the enclaves). The enclaves
from all three domes are composed mostly of plagioclase. The matrix is composed of
needle-like plagioclase grains of varying size. The needle-like grains rarely contain a
compositional rim or sieve-textures. Larger phenocrysts of plagioclase are also present in
the enclaves, although they are rare. These grains occasionally contain sieve textures and
deep embayments. The next most abundant phase in Bulalo and Olila is hornblende,
constituting 45% of the phenocrysts. Generally, the hornblende are anhedral and fill the
space between the plagioclase grains. However, some euhedral hornblende grains are
also present. Pyroxene is a rare phase in the enclaves of Olila and Bulalo. Both
hornblende and pyroxene are common phases in the Calamba enclaves. It is often
difficult to distinguish them visually because they fill the spaces between the plagioclase
grains, not allowing the use of cleavage planes or shapes to distinguish them visually.
Euhedral grains of pyroxene and hornblende are also present in the enclaves of Calamba,
although the type of pyroxenes present is unknown. Opaque grains occur in the enclaves
of all three domes.

Bulk Chemical Composition

Major elements

The Bulalo, Bijang and Olila domes have similar host compositions, whereas the
host composition of Calamba is distinctly different. The Calamba dome is dacitic (64-

66% 8102); whereas Bulalo, Bijang and Olila are dacitic to rhyolitic (69-73% $02)

12

(figure 9). Calamba also contains higher concentrations of A1203, F e203, MgO, and CaO
(figure 10). The mafic enclaves from Calamba, Olila and Bulalo are similar in
composition (figure 10), with a silica content of 50-55% (figure 9).

Trace elements

There is some variation in the trace element concentrations between Calamba and
the other three domes (figure 11). The concentration of Sr and Rb in the four domes is
very similar, while Calamba contains a much higher concentration of Y and Sm than the
other three domes. Calamba is also more enriched in the middle rare earth elements
(MREES) compared to the other domes. The chondrite normalized rare earth element
(REE) pattern for all of the domes is a concave upward trend. This trend is more
pronounced in Bulalo, Bijang and Olila than it is in Calamba (figure 12a). The difference
is also observed in a plot of Dy/Lu versus La/Lu (figure 12b), in which Dy represents the
MREEs. Olila, Bulalo and Bijang all have values between 0.6 and 0.87, falling below the
values of Calamba, 0.85 — 1.05. The MREES are strongly partitioned into arnphiboles,
with partition coefficients ranging from ~3 to ~13 (Rollinson, 1993). Therefore,
depletion in MREES is commonly attributed to the presence of amphibole in the source of
a magma. Y and Sm are also strongly partitioned into amphibole. The enclaves do not
show the depletion in MREEs, with Dy/Lu ratios greater than 1.0. Calamba contains a
higher concentration of the light rare earth elements (LREEs) (figure 12b) as well, with
La representing the LREEs on the diagram. None of the domes show a negative Eu
anomaly (figure 13). Sr has a high partition coefficient into plagioclase, and is

concentrated between 200-400 ppm in the host dome samples (figure 1 1).

13

Mineral Chemistry

Individual mineral phenocrysts were analyzed using EMPA. Grains analyzed
included plagioclase, hornblende, orthopyroxene, clinopyroxene, magnetite and ilmenite.
Points were taken in the center and edge of the plagioclase, as well as the area in-
between, where noted. If the plagioclase grain was small, points were labeled with
numbers, with the first point analyzed in the center of the grain and the second point
analyzed near the edge of the grain For all other mineral types, two points were
analyzed, typically one point near the center of the grain and one point near the edge of
the grain.

Plagioclase

The general trend for the host plagioclase grains is a decrease in anorthite (An)
content fiom center to edge. There were slight differences among the compositions of
the plagioclase grains from each dome despite this general trend. The An content of the
center of the plagioclase grains differed slightly between the domes, as did the
composition at the edge of the grains. The An content of the center of the well-zoned
plagioclase grains of Calamba are generally Am3-so (figure 14), although two grains
contain higher An concentrations in the center: Ana and A1184. The edges of all the
grains have An39.45. The well-zoned plagioclase grains of Bulalo contain centers with
concentrations similar to Calamba, Ammo, and edges of An33-37, slightly less than
Calamba (figure 14). One grain had a center as high as Anss, with an edge at Ansl. The
centers of the well-zoned plagioclase from Bijang cover a wider range of values than the
other two domes, with cores of M3643, and edges of ADM-41 (figure 14). Of the two well-

zoned plagioclase grains analyzed from Olila, one showed the common trend of

14

decreasing An, with a core of Anso and an edge of An” (figure 14). The other appears to
be reversely zoned, with a core of Am and edge of A1150. However, because this
plagioclase may be composed of several grains grown together, the apparent reverse
zoning trend may be the result of analyses that included more than one grain. One grain
from Bijang also shows this apparent reverse zoning, and also may be the result of
several grains grown together.

Bulalo and Olila are the only domes in which grains were analyzed from two
different sized enclaves. Plagioclase grains analyzed included the needle-like plagioclase
that composes the matrix, as well as larger phenocrysts. The compositions of the grains
are dependent on the size and shape of the grain, as well as the size of the enclave in
which the grain was located. In the Olila samples (figure 15), the plagioclase phenocryst
analyzed from the large enclave contain An90-93. The needle-like grains of the large
enclave contain Afl45.65. Grains were analyzed from what appeared to be a small enclave
in the host, but mixed results and the poor condition of the enclave lends doubt to that
interpretation. Of the three plagioclase grains analyzed fiom this area of the thin section,
one contained a core of A1134 and an edge of An54, one had points of M4045, similar to
grains in the host, and one contained a core of A1149 and an edge of An54. This grain had a
well-defined outer rim.

In the Bulalo samples (figure 15), the phenocrysts and needle-like plagioclase
from the larger enclave plot in the An65-7g range. Four grains were analyzed from the
smaller enclave in the host. The two needle-like plagioclase grains contained An7o.75,
while the two larger phenocrysts had centers at Ann and An45, and edges at Am, and

A1123.

IS

In the Calamba samples, only one large phenocryst and one needle-like
plagioclase grain were analyzed (figure 15). The larger phenocryst has a center with
Ango, and an edge at Ann. The needle-like plagioclase grain contains a concentration
around Ann as well. One analyzed grain (Enclave Plag #1-24) came from an area on the
thin-section interpreted to be part of a small enclave surrounded by the host, but it may
instead be part of a cumulate representing the magma chamber wall. Pyroxenes analyzed
from the same area of the thin section are not in equilibrium with the other pyroxenes in
the host, as determined using QUILF for therrnobarometry (see below). Despite this, the
plagioclase grain has a concentration of An4446, which is similar to the host plagioclase
grains.

The Ba concentrations in the plagioclase grains increase from center to edge,
whereas Sr decreases, which results a decrease in the Sr/Ba ratios across host plagioclase
from center to edge. The Sr/Ba ratios from the centers of the well-zoned plagioclase
from Calamba range from 2.2 to ~43, with edges decreasing to 2.2-3.0 (figure 16a). The
two grains with high An centers have identical Sr/Ba ratios of 6.2, and edges similar to
the other grains from Calamba The centers of the well-zoned plagioclase from Bijang
have Sr/Ba ratios between 2.2 and 3.4 (figure 16a), with the edges decreasing to around
1.9. The Sr/Ba ratios for the centers of the Bulalo plagioclase are 4.0 (figure 16a), with
the exception of one grain with a core at 6.0. The edges of the grains are all around 2.0.
While no well-zoned grains from Olila were analyzed for trace elements, one grain that
was analyzed across from rim to rim contained edge values at 2.7, and mid-points as high

as 4.0.

16

Two gains were analyzed from the smaller enclaves of both Olila and Bulalo
(figure 16b). The Sr/Ba ratios from the gains of the Olila enclave are ~40, similar to the
values of the plagioclase gains from host plagioclase. This supports the previous
conclusion that the area interpreted to be a small enclave most likely is not. The centers
of the Bulalo enclave plagioclase gains are 6.0 and 6.5, similar to the values of the
centers of the gains from Calamba and Bulalo with high An concentrations in the
centers. A point closer to the edge of one of the enclave gains shows a large decrease in
the Sr/Ba ratio, and plots with the edges of the host plagioclase gains.

Amphiboles

The arnphiboles analyzed from each dome are all homblendes based on their
composition. Ternary graphs of the major element concentrations of the arnphiboles
(figure 17a) show very little variation between the domes. The few amphibole gains
analyzed from the enclaves are similar in composition to the host amphiboles. A
comparison of magnesium numbers vs. SiOz between the hornblende gains from the
domes and the enclaves does not show a trend (figure 17b).

Pyroxenes

There is not much variation in the chemical composition of the pyroxenes among
the domes (figure 18a). A comparison of the amount of enstatite present in the pyroxene
gains with the Mg number of the gain also does not reveal a trend (figure 18b). All four
domes contain orthopyroxene of composition W013.” En6g_4.7o,6 F527,5-29,9. Calamba was
the only dome in which clinopyroxene (cpx) was observed and analyzed. It is possible
that the other domes also contain trace amounts of cpx, but none were observed with the

microprobe. The cpx present in the Calamba samples ranges from Wo4o,7.43,4 Em3_2.45,3

l7

F s 1 3.0.; 50. One gain contains a slightly different composition of W03“ Ens“ F5; 3,].
Thennobarometry could only be done for Calamba because of the lack of two different
types of pyroxenes in three of the domes,.

Calamba was also the only dome that contained both magretite and ilmenite, so
both of these systems were used to determine the final temperature of the Calamba
magna prior to eruption. Following the procedure outlined in Andersen et al. (1993),
QUILF version 4 was used to model the temperature. Of the gains analyzed, only two
were ilmenite, and the compositions of these two gains were different. The magnetite
gains also contained slightly different compositions, so several combinations of
magnetite and ihnenite were used in order to get the best results. The results are
summarized in Table 2. The calculated temperature was 854°C, with an uncertainty of
i64°C. The compositions of pyroxenes analyzed were also slightly different. The
temperature calculation that gave the least amount of error using only the pyroxene
system was 956°C, with an error of i15°C. Combining the two systems resulted in a
temperature of 749°C, and an error of i48°C. With such a wide range of calculated
temperatures, it seems likely that the minerals were not equilibrium with each other.
Therefore, the temperature cannot be accurately calculated.

Matrix Glass

Glass was analyzed from the matrix of the host samples as well as from the
enclaves of Bulalo and Olila. Generally, K20 content increased with increasing 8102
content, while MgO decreased with increasing 8102 (figure 19). The glass analyzed from
the enclaves had compositions that varied depending on the size of the enclaves. Glass

analyzed from the smaller enclaves from Bulalo and Olila contain $102, MgO and K20

l8

concentrations similar to the host matrix glass, indicating interaction between the host
and the intruding mafic magma. Glass analyzed from the large enclave from Olila
plotted in the low SiOz range of 52-55%, indicating little or no interaction with the high-
silica magna.

Oxygen Isotope Data

Data were collected from magnetite and hornblende gains from Calamba, Bijang
and Bulalo in order to determine the whole rock 8'80 values for each dome (table 3).
The 5'80 values collected from each mineral type were similar among the three domes
(figure 20). The magnetite values varied by less than 0.12 between Bulalo and Bijang,
and less than 0.5 for Calamba. The hornblende values were also very similar, with a
difference of less than 0.25 among all three domes. Whole rock 6180 values for the
domes were calculated using an assumed temperature of 950°C, following the procedure
from Clayton et al. (1989). The calculated whole rock 5180 values for the three domes
were also simlar. Bulalo contained 8180 of 5.9 %o, Calamba 6.29%», and Bijang was
measured at 6.06%o. The similarities of the 8180 values of the mineral phases and the
whole rock indicate that the minerals used in the calculations were in equilibrium with
each other. This is important because it indicates that oxygen values from the minerals
have not been reset, and therefore reflect the values of the source rock (Bindeman and

Valley, 2003).

19

DISCUSSION

Comparison of the Domes and Makiling

The domes from this study occur in close proximity to volcanic deposits from Mt.
Makiling. The domes are located on the south and southwest flanks of the mountain, and
the major element compositions are very similar to various Makiling deposits. The
majority of the volcanic products of Mt. Makiling are basaltic-andesite to andesite,
although smaller amounts of trachydacite and dacite compositions are also present (Cruz,
1992). Major elements of the samples from the domes overlap the composition of
samples from Makiling (figure 21a). The trace element compositions of the mafic
enclaves found in the domes and the low-silica samples of Makiling are also very similar
(figure 21b). The Silicic samples from Makiling do not have the same concave upward
trend in the REES that the domes have, indicating that the Makiling samples are not as
depleted in the MREES as the host dome samples. Cruz (1992) presented chemical
analyses of the lavas in the Mt. Makiling-Banahaw complex, and he concluded, based on
major and trace element variation, that the high-silica magnas of Makiling were related
to the low silica magnas through a process of fractional crystallization and assimilation.
He observed that fractional crystallization alone could not account for the chemistry of
the samples, including the high concentrations of Th, Ce, Zr, Hfand Sm. He proposed
that the assimilation of ~5% granite/upper crust compositions could account for this

composition.

20

Fractional Crystallization vs. Partial Melting

Several studies have examined the fractionation products of magna types
commonly found in are areas (figure 22). Grove et al. (2003) experimented with water-
saturated basalts at 200 MPa, while Muntener et al. (2001) experimented with basalts
containing 2 and 3% water and at 1 and 2 GPa of pressure (figure 22). Grove et al.
(2003) also modeled the fractionation of a water-saturated Mg-andesite at 200 MPa. One
of the difficulties in producing the Silicic magmas in the domes and Makiling is that the
K20/Na20 values are much higher than those produced in the experiments. One trend
that approaches the ratios of the domes and Makiling came from the fractionation of
water saturated Mg-andesite at a near-surface pressure (Grove et al., 2003 ). However,
the extensive fractionation required to produce high silica magnas would be unlikely to
have occurred at this shallow depth. Another trend that approaches the ratios of the
domes was produced through the anhydrous fractionation of a tholeiitic basalt at 1.0 GPa
(V illiger et al., 2004). However, these values were only reached after extremely high
amounts of fractionation had occurred, over 90%.

Board and Lofgen (1991) and Patino-Douce (2000) have examined the products
formed by the partial melting of various types of source rock. The products formed
through the melting of a meta-basalt (Patino-Douce, 2000) do not contain KZO/Nazo
ratios that are similar to the high-silica magnas from the domes and Makiling (figure 23).
Partial melting experiments beginning with meta-andesite to dacite compositions,
however, did produce products with ratios similar to the domes (Patino-Douce, 2000). In
this case, the KZO/NaZO values produced are high enough, but the NaZO + K20 is low.

Experiments in which the starting composition is a calk-alkaline andesite, such as those

21

found in the Corridor (Cruz, 1992) may be able to produce both the high KZO/NazO ratios
and the K20 + Na20 values of the domes. There have been no published experiments
involving the partial melting of calc-alkaline andesites similar to the ones found in the
Macolod Corridor.

Eu-anomalies are often used as an indicator of evolution by fractional
crystallization In order for sigrificant amounts of high-silica magna to be produced,
large amounts of plagioclase would have to be fractionated out (Price et al., 1999). This
would cause a noticeable negative Eu-anomaly. No negative Eu anomaly is observed in
the domes (figure 13). However, if the magnas were produced in an oxidizing
environment, Eu would occur as Eu”, and would not be partitioned into plagioclase.
Therefore, no negative Eu anomaly would be observed Because most arcs are oxidizing
environments, this may explain the lack of a Eu anomaly. Plagioclase fiactionation also
leads to a large depletion in the concentration of Sr in the more evolved samples because
Sr is strongly partitioned into plagioclase. Estimates of the partition coefficient for Sr
into plagioclase range from 2.8-15 .6 (Rollinson, 1993). The removal of the large
amounts of plagioclase required to reach high silica values should geatly deplete the
amount of Sr in these samples. The concentration of Sr in the host samples fall between
200 and 400 ppm, which seems to be too high to indicate evolution by fractional
crystallization (figure 13).

The composition of individual plagioclase gains has frequently been used to trace
processes occurring in magma chambers. The slow diffusion rate of Na and Ca through
the gains makes them an ideal indicator of how the chemistry of a magna changes

(Singer et al., 1995; Tepley III, et al., 1999; Ginibre et al., 2002; Browne et al., 2004).

22

The changing chemistry of a magna chamber should be recorded in the plagioclase
gains, with a high-anorthite core (An75-95) indicating the gain began gowing in a more
mafic magna, and decreasing anorthite towards the rim indicating a magna that is
becoming more Silicic (Gertisser et al., 2000). However, other processes occuning in the
magna chamber can affect the major element composition of the plagioclase gains,
including changes in water pressure and temperature, as well as magna mixing (Ginibre
et al., 2002; Browne et al., 2004). The trace element concentration in a gain, particularly
Ba and Sr, can help differentiate between these processes. The partitioning behavior of
Ba and Sr between liquids and plagioclase gains have been well-defined (Blundy and
Wood, 1991), and are not affected by the same processes as the major elements. Because
the Sr/Ba ratio reflects the change in anorthite across the gain (figure 24), the changes in
the chemistry of the gain are due to compositional changes in the magna chamber rather
than water pressure or temperature changes (Blundy and Wood, 1991; Browne et al.,
2004)

Fractional crystallization occasionally produces plagioclase gains with large
variations in An concentrations across the gain (>20%), and cores that indicate a mafic
origin for the gain (Singer et al., 1992; Watts et al., 1999; Gertisser et al., 2000). In
these studies, although these gains were present in the assemblages, they were rare. In
the dome samples, Calamba is the only one which contains plagioclase gains (2) that
have changes in An content of more than 20% from center to edge. In the other three
domes, no large changes in composition were observed. The Sr/Ba ratio in the cores of

the gains would also record an origin in a less evolved magma. Only 3 gains in the host

23

domes contain centers with much higher Sr/Ba ratios than the other host gains- the 2
gains from Calamba and one from Bulalo (figure 16a).

Magma mixing

Mingling and mixing between the more mafic magna represented by the enclaves
and the host silicic magnas of the domes did not play a major role in the generation of
the dome magnas. The chemical compositions of the minerals do not indicate much
interaction between the silicic host and more mafic magna. There is no evidence that
gains were shared between the two magna types, as would be expected if they had been
in contact for a sigrificant amount of time (Snyder and Tait, 1998). Also, reversely-
zoned plagioclase gains are not found in the host, and normally zoned plagioclase that
show a geat decrease in An content from the center to the edge are very rare. The rims of
the plagioclase are in equilibrium, as indicated by the similar composition, and do not
contain the increase in anorthite content or Sr/Ba that would be observed due to
prolonged contact with a mafic magna.

There is also little textural evidence for magna mixing. Sieve textures and
reaction rims on minerals are very rare in the samples, except along boundaries between
the host and enclave, as well as in the smaller enclaves. Also, analyses taken from these
sieve-textured cores, including the An-content and Sr/Ba ratios, were not different from
the cores of the other gains (e. g. Calamba Plag #1-24). This compositional similarity
indicates that the sieve-textured cores present may be the result of other processes in the
magna chamber that caused disequilibrium between the gain and the liquid, and lead to
partial dissolution of the gain. These processes could include a change in temperature or

pressure within the chamber. The rims that are present on the plagioclase gains are thin,

24

even along the boundaries between the enclaves and host. The widest rims are found in
the smaller enclaves, indicating more interaction with the host. There is no evidence of
mingled glass in the host. The glass analyses from the matrix of the host contain a 8102
content that is higher than the bulk $102 content (figure 19). Glass analyzed from the
larger enclave of Olila has a 8102 content that was similar to the bulk silica content of the
enclave, indicating little, if any interaction with the host magna Glass analyzed from
the smaller enclaves contained much higher Si02 values, indicating more interaction with
the silicic magna.

Eruption of the magma/formation of the domes

I propose a model for the formation of the dome and the high-silica Makiling
magnas involving the Mal melting of discrete batches of previously emplaced calc-
alkaline andesitic magna(fig1re 25). In this model, the first step involves melting of the
mantle wedge as the result of the subduction of the Eurasian plate. The magnas
produced in this manner travel through the wedge and pond at the base of the lower crust,
where they may remain partially molten. From experimental petrology, we know that
basaltic magnas could not produce the composition of the dome magnas, it is likely that
these ponded, crystallized magna batches are calc-alkaline andesite (or dacite) in
composition. In the next step, influxes of basaltic magna produced in the mantle wedge
encounter the solidified magna body, partially melt it, and mobilize the more silicic melt.
This siliceous melt travels through the crust and forms a magna chamber, possibly in the
upper crust. There is little interaction between the silicic magna in the chamber and the
wall-rock surrounding it, because interaction with rocks in the upper crust would raise the

oxygen isotope ratios to values above the mantle values observed in the dome samples

25

(Bindeman and Valley, 2003). In the third step, hot, mafic magna is injected into the
silicic magna chamber, causing a rapid eruption due to an increase in pressure and
temperature in the magna chamber. The extensive faulting in the Macolod Conidor
most likely creates weaknesses in the crust, making it easier for the magnas to reach the
surface. These magnas then erupt, forming the domes. The contact between the mafic
and silicic magna in the chamber is relatively brief, as the lack of any evidence of
mingling or mixing between the two magna types suggests.

The processes that formed the four domes examined in this study were probably
very similar, which led to the similar chemical compositions and mineral textures among
the four domes. The differences between Calamba and the other three domes could be
the result of source magnas with different chemical compositions, or different processes.
However, the similar 8180 values among Bulalo, Olila and Calamba suggest that each
originated from a similar source. One difference between them may be the depth that
each magna formed at, because amphibole has a very strict depth limit at which it can
form. Because Bulalo, Olila and Bijang all contain sigrificant amounts of amphibole, it
is also possible that the source magnas for those three domes were more hydrous than
the magna of Calamba. One other possibility is that the Calamba magna formed due to
higher degees of partial melting. The lower concentrations of silica, and higher
concentrations of A1203, MgO, FeO, CaO and NaZO support this. The higher Dy/Lu
ratios of the Calamba samples provide further evidence of a higher degee of partial
melting, providing that the source contains large amounts of amphibole. Higher degees
of partial melting of an arnphibolitic source would lead to a geater concentration of

MREEs in the resulting magna. More partial melting of a source would also lead to a

26

lower concentration of LREEs. An initial melt would be highly concentrated in the
incompatible LREEs, which would become more dilute after further partial melting
events.

The domes and the high-silica magna from Makiling are most likely not related.
The lack of similarities between the trace elements of the domes and Makiling indicates
that while it’s possible that the processes that formed them were similar, it is likely that
the source magnas were different. Further data collection could determine more exactly

how these areas are related, particularly oxygen isotope data from the Makiling silicic

magnas.

27

CONCLUSION

The majority of the evidence presented in this study indicates that partial melting
of previously emplaced discrete andesitic bodies located in the lower crust formed the
high-silica magnas of the domes. Fractional crystallization of a magna body can not
account for the compositions of the dome magnas. The KZO/NazO ratios can not be
reproduced by fractional crystallization alone. The Sr values of the whole rock are too
high to account for the large amounts of fractionation required to form sigiificant
amounts of high-silica magna Textural and chemical data do not indicate that magna
mixing and mingling played a major role in the creation of the dome magnas. They
show, instead, that the mafic magnas represented by the enclaves were not in contact

with the silicic magna for a sigrificant length of time.

28

APPENDIX 1

PETROGRAPHIC DESCRIPTIONS

29

Petrographic Analyses

Bijang

The samples from Bijang are porphyritic, with 15-25% phenocrysts and a glassy,
microlitic matrix. Plagioclase is the most abundant mineral in Bijang, constituting
around 60% of the phenocrysts. The phenocrysts range in size from 0.2 to 2.7 mm, with
an average of approximately 1 mm and a normal gain-size distribution. Any plagioclase
gain with a length less than 0.1 mm was considered part of the matrix (in all four
domes). The gains are mostly twinned and euhedral with most showing rounded edges
and slight embayments, which may indicate partial resorption. Grains with a sieve
texture throughout are rare. Most of the larger gains are well-zoned, and some of the
smaller gains also show zoning. Rarely, gains show a sieve texture core and a well-
zoned rim. Glomerophyric clots consisting of two or more gains of plagioclase that have
gown together are present in the samples. In these clusters, the outer edges of the
plagioclase contain slight resorption features. These clusters occasionally contain other
minerals, including amphibole and opaques. These may be pieces of the wall rock that
were taken up during the eruption and not part of the host magma.

Homblende is the next most abundant phenocryst, constituting about 30% of the
phenocrysts. The gains are mostly euhedral with some subhedral gains. They range in
size from 0.13 to 0.7 mm, although the larger gains are rare. Most are in the 0.2-0.4 mm
range. Smaller gains are present in the matrix (< 0.1mm), but in much smaller quantities
than the plagioclase. The hornblende gains often display some resorption features, with

rounded edges and slight embayments. Homblende gains with disequilibrium textures

30

such as an extremely sieved texture and large embayments are rare. Reaction rims were
not observed on the hornblende gains.

Opaque gains are found throughout the samples, in the matrix as well as in
phenocrysts as inclusions, and constitute ~5% of the phenocrysts. The shapes vary from
euhedral to anhedral, and the gains do not contain embayments. The larger gains are
approximately .66 mm, although most are much smaller. Orthopyroxene is the least
abundant mineral in Bijang, composing 3-4% of the phenocrysts. The gains range in
size fiom 0.28 mm to less than 0.06 mm. The larger gains are rare, and most of the
gains are around 0.1 mm or smaller. The pyroxenes are mostly euhedral and few show
sigrs of resorption. Biotite is also present in the samples in very trace amounts, as

inclusions in the hornblende.

Bulalo

The mineralogy of Bulalo is very similar to Bijang, although Bulalo contains
mafic enclaves. The samples from Bulalo are porphyritic, with a phenocryst content of
20-25% and a glassy, microlitic matrix. The matrix contains brownish areas that most
likely are areas of devitrification. Plagioclase is the most abundant phase, constituting
«65% of the phenocrysts. The phenocrysts range in size from 0.17 to 2.16 mm, with an
average of ~1 mm and a normal gain-size distribution. The gains are commonly
twinned, and are euhedral to subhedral. Many show slight resorption features, such as
rounded edges and slight embayments. Grains with a sieve texture are present, but rare.
Grains with sieve-textured cores and well-zoned rims are also rare. Zoning is common in

the gains, especially in the smaller ones. Some gains display well-developed outer rims

31

that may represent contact with a magna of a different composition, but these are not
common in the host plagioclase. Glomerophyric clots consisting only of plagioclase are
present but rare, as are clots containing other mineral types. These minerals include
hornblende, magnetite, and orthopyroxene (as rare inclusions in the hornblende).

Homblende is the second most abundant phase, constituting about 25% of the
samples. The gains are euhedral to subhedral. The homblendes range in size from about
0.18 to 0.70 mm with an average of 0.25 mm. Larger gains of hornblende are rare.
Smaller gains are found in the matrix. Many of the non-matrix hornblende gains show
sigrs of resorption, including rounded edges and slight embayments. The homblendes
rarely contain a sieve texture in the core, or throughout the gain. Reaction rims were not
observed on the hornblende gains.

Orthopyroxene constitutes ~5% of the phenocrysts. The gains range in size from
0.05 mm to 0.27 mm, although most of the gains are small, between 0.08 and 0.1 mm.
The gains are mostly euhedral and show little evidence of resorption. The resorption
features are more common in the large gains than the small ones. Opaque gains
compose 3-4% of the samples. The shapes of the opaques range from euhedral to
anhedral. The gains are not embayed. The largest gains are around 0.32 mm, with an
average of 0.05 mm.

The mafic enclaves found in Bulalo are various sizes, but the mineralogy is the
same. Some of the enclaves are fist-sized and could be sampled individually, composing
the mafic samples from Bulalo. Some of the enclaves are very small, and are included in
the host samples. The enclave features a noticeable change in texture from the host, with

the matrix being composed of needle-like plagioclase, with sizes from 0.46 mm to

32

<0.1mm. The average size is ~0.3 mm. The smaller enclaves contain matrix plagioclase
that are generally smaller, 0.39 mm long and 0.09 mm wide. The gain size is the only
difference among the different sized enclaves. The mineralogy is the same, with 50%
plagioclase, 45% hornblende and 5% opaques. Some of the plagioclase gains show
distinct rims. Larger, plagioclase phenocrysts are present in the enclave, but rare. These
are up to 0.39 mm long. The hornblende in the enclaves is almost as abundant as the
plagioclase, with a size range that is from 0.03 mm to 1.25 mm. Many of the gains are
anhedral and fill in the space between the plagioclase gains, while others have an
elongate, euhedral shape. Some of the hornblende gains have a sieve texture, although
this is not common. Opaque gains are scattered throughout the enclave, and constitute
~5% of the phenocrysts. The size and shape of the opaques vary, with no dominant
shape. The average size is around 0.05 mm. There are no resorption features on these

gains. Glass is present in small amounts in the enclaves.

Olila

The samples from Olila are porphyritic, with phenocrysts constituting 20-25% of
the samples, and a glassy, microlitic matrix. Mafic enclaves are also present in the Olila
samples. There are some brown areas that may be the result of devitrification.
Plagioclase is the most abundant phase, constituting ~68% of the phenocrysts. The
gains range from 0.15 to 2.16 mm, with an average of ~1 mm and a normal gain-size
distribution. Most of the gains are twinned and euhedral, and most show sigrs of
resorption. Some plagioclase gains are subhedral due to what appears to be deep

embayments. A few gains in the host also display cores with sieve textures and well-

33

zoned rims. Some appear to have well-developed outer rims on them. Most occur as
single gains, with rare glomerophyric clots consisting of only plagioclase. Clots
containing plagioclase, hornblende, opaques and orthopyroxene are rare as well. They
may represent wall rock from the chamber.

Homblende constitutes ~ 25% of the phenocrysts in Olila. The gains are
generally euhedral, although most of them have rounded edges and slight embayments.
The hornblendes have a large range, from ~ 0.09 to 2.0 mm. They average 0.9 to 1.1
mm. Small (< 0.1 mm) gains were observed in the matrix. The non-matrix hornblende
gains rarely contain a sieve texture throughout. Most of the large gains contain
inclusions of plagioclase and opaques. No reaction rims were observed on the
hornblende gains of Olila.

The opaque gains make up 5% of the phenocrysts of Olila. They are found in a
variety of shapes, ranging from euhedral to anhedral. The gains do not typically contain
embayments, although some were observed on the larger gains. The larger gains are
approximately 0.32 mm in diameter, although most are much smaller. Orthopyroxene is
the least abundant phenocryst in Olila, constituting ~3% of the phenocrysts. The gains
range in size fi'om 0.04 mm to ~0.58 mm, although the larger pyroxenes are rare. Most
of the gains are 1 mm or less. The shapes of the gains are euhedral to subhedral, and
slight embayments occur rarely.

The Olila samples contain enclaves of varying sizes with a mineralogy similar to
the enclaves of Bulalo. The mineralogy of the different sized enclaves is the same, but
the gain sizes are slightly different Generally, the matrix of the enclaves is composed of

needle-like plagioclase gains. The lengths of the matrix plagioclase of the larger

34

 

(IO

N0

Cale

enclaves range from 0.07 to 0.62 mm, with widths from 0.02 to 0.05 mm. In the smaller
enclaves, the lengths of the needle-like plagioclase range from 0.04 to 0.2 mm and widths
range from 0.006 to 0.008 mm. Some of the needle-like plagioclase of the smaller
enclaves contain a noticeable rim. These are rare in the larger enclaves. The plagioclase
phenocrysts present in the smaller enclaves are not common. They are generally ~ 0.72
mm and show some zoning. Altogether, plagioclase constitutes ~50% of the minerals.
Homblende is also found in the enclave, composing ~50% of the phenocrysts. Most of
the hornblende is anhedral and fills the space between the plagioclase gains. Opaque
gains in the enclaves range in size from 0.02 to 0.08 mm. These gains are generally
anhedral-subhedral, with some euhedral gains, and constitute only ~1% of the

phenocrysts.

Calamba

The samples from Calamba are porphyritic, with phenocrysts constituting ~20-
25% of the samples. The matrix is devitrified in most of the samples, although one
sample (020517—2d) does contain a glassy matrix. Mafic enclaves are present in the
Calamba samples. Generally, the phenocrysts in Calamba compose around 20-25% of
the sample. Plagioclase is the most abundant phase, composing 70% of the phenocrysts.
Grain-sizes of the plagioclase are normally distributed, and range from 0.08 to 2.37 mm,
with an average size of 1.2 mm. Many of the gains are twinned, and most show sigis of
resorption, including rounded edges and slight embayments. Grains with a sieve-texture
core with a well-zoned rim were rare. Grains that were completely composed of a sieve

texture are also rare. In the Calamba samples, glomerophyric clots consisting only of

35

plagioclase gains are rare. However, clots consisting of plagioclase, clinopyroxene,
opaques and orthopyroxene are common. These clots may represent pieces of the wall
rock that were taken into the host magna. The size and shape of the gains in these clots
is variable. Some of them contain large plagioclase gains, with all the remaining gains
being much smaller. Others have large clinopyroxene and small plagioclase gains. The
cumulates appear to have disaggegated.

The next most abundant phase is pyroxene, which constitutes 25% of the
phenocrysts. Both clinopyroxene and orthopyroxene are present, but it is difficult to
distinguish the two under the microscope. Grain size ranges from 0.05 mm to ~ 0.23
mm. Most of the gains are small, with the average of approximately 0.12 mm.
Generally, the individual gains are euhedral and show no sign of resorption. However,
the larger gains are often subhedral. This is possibly due to resorption, or they may be
part of the disagge gated cumulate.

The next most abundant phase in Calamba is the opaque gains, constituting 3-
4% of the phenocrysts. The gains are mostly anhedral to subhedral, with a few euhedral
gains observed. Grain size ranges from 0.03 to 0.43 mm. Both magretite and ilmenite
are present in the samples, but they are impossible to distinguish under the microscope.
The gains did not show resorption features. Homblende is a rare phase in the host, with
only a few gains identified. Those present are small (< 0.05 mm) and subhedral-
anhedral.

The mafic enclaves in the Calamba samples contain a mineralogy that is different
than the other three domes. The minerals present include plagioclase, hornblende,

pyroxene and opaques. The matrix is composed of needle-like plagioclase. Along the

36

edge of the enclave that is in contact with the host, the plagioclase gains are much
smaller, with sizes around 0.04 mm long and only 0.008 mm wide. Farther away from
the contact zone, the plagioclase are larger, approximately 0.12 mm wide and 0.83 mm
long (on average). Resorption features and well-defined outer rims are common on the
plagioclase in the enclave. The larger phenocrysts of plagioclase in the enclaves are
often severely resorbed, with sieve textures and deep embayments. Some of the gains
have a core with a sieve texture, and a rim that is severely embayed.

The pyroxenes and hornblende in the enclaves are anhedral, and appear to have
gown between the plagioclase. This makes it difficult to distinguish them visually
because the cleavage planes and shapes are often missing or distorted. They are found in
a much smaller abundance than the plagioclase, and often display a sieve texture.
Euhedral gains of pyroxene and hornblende are present, but rare. Many opaques are
present in the enclaves, but they are often very small. They have variable shapes, and

some have a reddish tint around them.

37

APPENDIX 2

FIGURES

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Figure 1— Map of the Philippines showing the location of the plates and the
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39

 

 

 

 

 

Figure 2- Location of the Macolod Corridor: It is located between the
Bataan and Mindoro segments of the Luzon Are. On this diagram,
the Eurasian Plate has been labeled as the South China Sea
Plate. The Mindoro-Palawan terrane in the southwest part of the
islands contains a large block composed of continental crust.
However, it is located well south and west of the Macolod Corridor,
in which the presence of continental crust has not been observed
(Defant et al., 1989).

40

 

 

 

 

 

Figure 3- Location of the Macolod Corridor in relation to Taal
Volcano and the Laguna de Bay caldera (Sudo et al., 2001).

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Figure 25- Partial melting and eruption model- a. Dehydration
melting of the mantle wedge leads to the formation of a mafic
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encounters a solidified or partially solidified body of calc-alkaline
andesite. The heat from the mafic magma partially melts and
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requiring an additional influx (b) of hot, mafic magma to cause the
eruption. (Not to scale)

APPENDIX 3

TABLES

67

Table 1- Ages of Selected Domes from the Macolod Corridor

Location
T 43 :t 13

Bulalo 15:7
66:14

 

(Source: Heizler, personal communication, 2003)

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Table 3- Oxygen Data

 

 

 

 

 

 

 

 

 

 

Bulalo Calamba Bijang
Whole Rock 5.90 6.29 6.06
2.83 (1
Mneflte 2.36 t .08 analysis) 2.48 i .12
Homblende 4.90 :l: .03 4.82 :t .14 4.67 1: .06
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8.8 8.8 8.0 8.0 8.0 8.8 «0.0 8.0 8.« 8.2 3.8.8 «.2... 8&8: 8283
8.8 8.2 8.0 8.0 8.0 8.8 «0.0 8.0 8.« 8.2 88.8 2.88.... 638.283
««.8 8.8 8.0 «0.0 8.0 8.3 8.0 2.0 8.2 8.2 0.8.8 38... 9,9828. 8.383
3.8 8.8 8.0 2.0 8.0 :3 8.0 2.0 :2 3.2 0.8.8 8 8.... 988.8. 8.383
2.8 2.8 8.0 20.0 8.0 8.3 20.0 «2.0 3.2 3.2 0.203 8858088303
88 8.3 3.0 20.0 3.0 33 20.0 2.0 :2 8.2 0.98 885808-383
8.8 8.8 8.0 8.0 3.0 83 20.0 «2.0 2.2 8.2 0.3.8 8858088303
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8.8 8.5 8.0 55 3.0 8.0 So 8.0 :.~ :2 2:0 885858-888
8.8 8.8 8.0 8d 8.0 88 5o mod 3a 8a «...0 3836039888
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8.8 8.8 2.0 8.0 93 88 mod :d 8.« 8., «so 885858-888
8.8 8.8 2.0 8.0 3° .3 8d :d 8.« 8; 2:0 8 856038-888
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94

Table 9a— Trace Elements- Plagioclase

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

samme Dome Ba Sr CaO Sr/Ba %An
020518-1c(15) plgg#2-oore Bijarlg 454.76 1107.77 8.07 2.44 38.65
020518—1c (15) pla£#2-mid1 Bijang: 483.71 1172.92 8.22 2.42 39.19
020518-1c (15) plgg#2-mid2 Bijang 700.15 1198.92 7.80 1.71 37.65
020518-1c (15) plag #2-edge Bijang 559.65 1080.12 8.00 1.93 38.14
020518-1c (15) plag #4-core Bijang 216.32 755.79 10.08 3.49 47.48
020518-1c (15) plaggM-mid Bijang 382.48 714.68 7.21 1.87 34.41
020522-51 (94) pl_ag #2-core Bulalo 192.33 1166.58 1 1.16 6.07 55.27
020522-51 (94) mam-rim Bulalo 634.50 1455.1 1 10.47 2.29 51 .82
020522-51 (94) plggM—core Bulalo 282.31 1122.49 9.98 3.98 47.88
020522—51 (94) plag#6 core-a Bulalo 327.45 1343.83 9.58 4.10 46.02
020522-51 (94) plagiG—mid Bulalo 366.27 971.77 7.00 2.65 33.76
020522-51 (94) 9'39 #6-rim Bulalo 519.38 967.63 7.01 1 .86 33.81
020517-2d (24) plag #1 -core Calamba 296.64 965.87 9.32 3.26 44.56
020517-2d (24) p199 #1 -n'm Calamba 298.99 841.89 8.39 2.82 40.37
020517-2d (24) plal#3—core Calamba 267.32 1657.04 16.81 6.20 82.94
020517-2d (24) plag #3-mid Calamba 237.63 1136.34 12.12 4.78 59.15
020517-2d (24) pl§g#3-rim Calamba 372.01 899.07 8.32 2.42 40.42
020517-2d (24) plag#5—core Calamba 233.14 1024.65 10.18 4.39 49.08
020517-2d (24) plagi5-mid Calamba 340.56 973.69 8.67 2.86 41.80
020517-2m (31) plaggfl-core Calamba 320.65 1046.02 9.73 3.26 46.66
020517-2m (31) plagm-mid Calamba 255.34 944.20 9.17 3.70 43.66
020517-2m (31 ) plag#1-rim Calamba 392.80 1019.35 9.27 2.60 44.51
020517-2m (31) plag#3-oore Calamba 205.49 1261.65 13.36 6.14 64.41
020517-2m (31 ) plag #3-mid1 Calamba 270.20 1069.61 9.60 3.96 46.68
020517-2m (31) glafl3-mid2 Calamba 488.70 1 167.35 10.10 2.39 48.79
020517-2m (31) 9ng #3—rim Calamba 388.68 960.22 8.92 2.47 42.63
020517-2m (31) plag #4—core Calamba 350.01 823.1 1 8.85 2.35 42.97
020517-2m (31) plag#4—mid Calamba 400.30 958.72 8.56 2.39 41.07
020517-2m (31) plag #4—rim Calamba 351.92 905.17 8.91 2.57 43.06
Table 9!)- Trace Elements— Enclave Plagioclase
sample Dome Ba Sr 030 Sr/Ba %An
020522-51 (94)plag;#8-oore Bulalo 181 .27 1 192.05 14.91 6.58 73.07
020522-51 (94) plag#10—oore Bulalo 142.74 880.49 9.29 6.17 46.12
020522-51 (94)ng #10mid Bulalo 490.34 1012.58 7.03 2.07 34.39
020522-53 (100) plag #6-core Olila 574.66 2230.81 10.66 3.88 50.98
020522-53 (100) plain—core Olila 378.23 1567.02 9.91 4.14 47.05

 

 

 

 

 

 

 

95

 

 

REFERENCES CITED

Andersen, D.J., Lindsley, DH. and Davidson, PM, 1993, QUILF: A PASCAL program
to assess equilibria among Fe-Mg-Mn-Ti oxides, pyroxenes, olivine, and quartz,
Computers and Geosciences, 19, 9: 1333-1350

Aquino, D.J.P, 2004, Surface Structure Analysis for the Bulalo Geothermal Field:
Possible Implications to Local and Regional Tectonics, MS thesis, University of
the Philippines: 116 pp.

Bates, KL. and Jackson, J .A. (eds), 1957, Dictionary of Geological Terms, American
Geological Institute, New York: 571 pp.

Bautista, B.C., Bautista, M.L.P., Oike, K., Wu, PT and Punongbuyari, RS, 2001, A
new insight on the geometry of the subduction slabs in northern Luzon,
Philippines, Tectonophysics, 339: 279-310

Beard, J .S. and Lofgren, GE, 1991, Dehydration melting and water-saturated melting of
basaltic and andesitic greenstones and amphibolites at 1, 3, 6 and 9 kbar, Journal
of Petrology, 32: 365-401

Bindeman, IN. and Valley, J .W., 2003, Rapid generation of both high- and low-8180,
large volume silicic magmas at the Timber Mountain/Oasis Valley caldera
complex, Nevada, GSA Bulletin, 115, 5: 581-595

Blundy, J .D. and Wood, B.J., 1991, Crystal-chemical controls on the partitioning of Sr
and Ba between plagioclase feldspar, silicate melts, and hydrothermal solutions,
Geochimica Acta Cosmochimica, 55: 193-209

Brophy, J .G., and Dreher, S.T., 2000, The origin and composition gaps at South Sister
volcano, central Oregon: implications for fractional crystallization processes
beneath active calc-alkaline volcanoes, Journal of Volcanology and Geothermal
Research, 102: 287-307

Browne, B.L., Eichelberger, J .C., Patino, L.C., Vogel, T.A., Uto, K. and Hoshizumi, H.,
2004, Magma mingling as indicated by texture and geochemistry of plagioclase
phenocrysts from Unzen Volcano, SW Japan, Journal of Volcanology and
Geophysical Research, in review

Cardwell, R.K., Isacks, BL. and Karig, DE, 1980, The spatial distribution of
earthquakes, focal mechanism solutions and subducted lithosphere in the
Philippine and Northeastern Indonesian Islands, in Hayes, D.E. (ed), The Tectonic
and Geologic Evolution of Southeast Asian Seas and Islands, Geophysical
Monograph 23: 1-35

96

Catane, S.G. and Arpa, CB, 1998, Large-scale eruptions of Laguna caldera:
contributions to the accretion and other geomorphic developments of Metro
Manila and adjacent provinces. PI-IIVOLCS internal report.

Clayton, R.N., Goldsmith, J .R. and Mayeda, T.K., 1989, Oxygen isotope fractionation in
quartz, albite, anorthite, and calcite, Geochimica Acta Cosmochimica 53, 3: 725-
733

Cruz, J .B., 1992, Petrology and geochemistry of lavas from the Makiling-Banahaw
volcanic complex, Southern Luzon, Philippines, M.S. thesis, University of
Illinois, Chicago, IL

Defant, M.J., Jacques, D., Maury, R.C., Boer, J .D. and Joron, J-L., 1989, Geochemistry
and tectonic setting of the Luzon Arc, Philippines, Geological Society of America
Bulletin, 101: 663-672

Gertisser, R. and Keller, J, 2000, From basalt to dacite: origin and evolution of the calc-
alkaline series of Salina, Aeolian Arc, Italy, Contributions to Mineralogy and
Petrology, 139: 607-626

Ginibre, C., Womer, G. and Kronz, A., 2002, Minor- and trace-element zoning in
plagioclase: implications for magma chamber processes at Parinacota volcano,
northern Chile, Contributions to Mineralogy and Petrology, 143: 300-315

Grove, T.L., Elkins-Tanton, L.T., Parman, S.W., Chatterjee, N., Muntener, O. and
Gaetani, GA, 2003, Fractional crystallization and mantle melting controls on
calc-alkaline differentiation trends, Contriubtions to Mineralogy and Petrology,
145: 515-533

Hannah, R.S., Vogel, T.A., Patino, L.C., Alvarado, G.E., Perez, W. and Smith, DR,
2002, Origin of silicic volcanic rocks in Central Costa Rica: a study of a
chemically variable ash-flow sheet in the Tiribi Tufi’, Bulletin of Volcanology, 64:
117-133

Heizler, M., 2003, 4OAr/39Ar geochronology results for volcanic rocks from the
Philippines, Internal report NMGRL—IR-3 02&341 prepared for the New Mexico
Geochronological Laboratory

Knittel, U., Defant, M.J. and Raczek, 1., 1988, Recent enrichment in the source region of
arc magmas from Luzon island Philippines: Sr and Nd isotopic evidence,
Geology, 16: 73-76

LeBas, M.J., LeMaitre, R.W., Streckeisen, A., and Zanettin, B., 1986, A chemical

classification of volcanic rocks based on the total alkali silica diagram, Journal of
Petrology, 27: 745-750.

97

Mukasa, S.B., Flower, MR]. and Miklius, 1994, The Nd-, Sr- and Pb-isotopic character
of lavas from Taal, Laguna de Bay and Arayat volcanoes, southwestern Luzon,
Philippines: Implications for are magma petrogenesis, Tectonophysics, 235: 205-
221

Muntener, O., Kelemen, PB and Grove, T.L., 2001, The role of H20 during
crystallization of primitive arc magmas under uppermost mantle conditions and

genesis of igneous pyroxenites: an experimental study, Contributions to
Mineralogy and Petrology, 141, 6: 643-658

Oles, D., 1991, Geology of the Macolod Corridor intersecting the Bataan-Mindoro island
arc, The Philippines, Final report for German Research Society Project No.
F053/16-1 to 2 and German Agency for Technical Cooperation Project No.
85.2522.2-06. 100

Price, R.C., Stewart, R.B., Woodhead, J .D. and Smith, I.E.M., 1999, Petrogenesis of
high-K arc magmas: Evidence from Egmont Volcano, North Island, New
Zealand, Journal of Petrology, 40, 1: 167-197

Riley, T.R., Leat, P.T., Pankhurst, RJ. and Harris, C., 2001, Origins of large volume
rhyolitic volcanism in the Antarctic Peninsula and Patagonia by crustal melting,
Journal of Petrology, 40, 1: 1043—4065

Rollinson, H., 1993, Using geochemical data: evaluation, presentation interpretation,
Longrnan Group, UK: 352 pp.

Singer, B.S., Myers, J .D. and Frost, CD, 1992, Mid-Pleistocene lavas from the Seguam
volcanic center, central Aleutian are: closed system fractional crystallization of a
basalt to rhyodacite eruptive suite, Contributions to Mineralogy and Petrology,
42, 6: 1043-1065

Singer, 88., Dungan, MA. and Layne, GD, 1995, Textures and Sr, Ba, Mg, Fe, K, and
Ti compositional profiles in volcanic plagioclase: Clues to the dynamics of calc-
alkaline magma chambers, American Mineralogist, 80: 776-798

Smith, I.E.M., Stewart, RB. and Price, R.C., 2003a, The petrology of large intra-oceanic
eruption: the Sandy Bay Tephra, Kennadec Arc Southwest Pacific, Joumal of
Volcanology and Geothermal Research, 124: 173-194

Smith, I.E.M., Worthington, T.J., Stewart, R.B., Price, RC. and Gamble, J .A., 2003b,
Felsic Volcanism in the Kennadec arc, SW Pacific: crustal recycling in an
oceanic setting, in Larter, RD. and Leat, P.T., (eds), Intra-Oceanic Subduction

98

Systems: Tectonic and Magmatic Processes, Geological Society of London
Special Publications, 219: 99-118

Snyder, D. and Tait, S., 1998, The imprint of basalt on the geochemistry of silicic
magmas, Earth and Planetary Science Letters, 160, 3-4: 433-445

Sudo, M., Listanco, B.L., Ishikawa, N., Tagami, T., Kamata, H. and Tatsumi, Y., 2001,
K-Ar dating of the volcanic rocks from the Macolod Corridor in Southwestern
Luzon, Philippines: Toward an understanding of the Quaternary volcanism and
tectonics, Journal of the Geological Society of the Philippines, 55, 1-2: 89-104

Sun, S. and McDonough, W.F., 1989, Chemical and isotopic systematics of oceanic
basalts: implications for mantle compositions and processes in Saunders, AD.
and Norry, M.J. (eds), Magmatism in the Ocean Basins, Geological Society
Special Publication No. 42: 313-345

Tamura, Y and Tatsumi, Y, 2002, Remelting of an andesitic crust as a possible origin for
rhyolitic magma in oceanic arcs: an example from the Izu-Bonin Arc, Journal of
Petrology, 43, 6: 1029-1047

Tamura, Y., Yuhara, M., Ishii, T., Irino, N. and Shukuno, H., 2003, Andesites and
Dacites from Daisen Volcano, Japan: Partial-to-total remelting of an andesite
magma body, Journal of Petrology, 44, 12: 2243-2260

Tepley 111, El, Davidson, J .P. and Clynne, MA, 1999, Magmatic interactions as
recorded in plagioclase phenocrysts of Chaos Crags, Lassen Volcanic Center,
California, Joumal of Petrology, 40, 5: 787-806

Watts, R.B., de Silva, S.L. and de Rios, G.J., 1999, Effusive eruption of viscous silicic
magma triggered and driven by recharge: a case study of the Cerro Chascon-

Runtu Jarita Dome Complex in Southwest Bolivia, Bulletin of Volcanology, 60:
241-264

Viray, E., 2003, Origin and evolution of the Nicaraguan silicic ash-flow sheets, MS.
Thesis, Michigan State University, East Lansing, MI

99

     
 

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